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Digitized by the Internet Archive 
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 https://archive.org/details/geologypalontolo9218jack 
 
THE 
 
 GEOLOGY AND PALAONTOLOGY 
 
 OF 
 
 QUEENSLAND 
 
 AND 
 
 NEW GUINEA, 
 
 WITH SIXTY-KIGHT PLATES AND A GEOLOGICAL MAP OF QUEENSLAND. 
 
 BY 
 
 ROBERT L. JACK, F.G.S., F.R.G.S., 
 
 GOVERNMENT GEOLOGIST FOR QUEENSLAND; FORMERLY OF THE GEOLOGICAL SURVEY OF SCOTLAND ; 
 
 no 
 
 AND 
 
 ROBERT ETHERIDGE, JUNIOR, 
 
 GOVERNMENT PALHONTOLOGIST (NEW SOUTH WALES); FORMERLY ASSISTANT-GEOLOGIST, GEOLOGICAL SURVEY OF 
 VICTORIA ; ACTING-PALHZONTOLOGIST, GEOLOGICAL SURVEY OF SCOTLAND; AND SENIOR 
 ASSISTANT, DEPARTMENT OF GEOLOGY, BRITISH MUSEUM, LONDON, 
 
 
 
 PUBLISHED UNDER THE AUTHORITY OF THE HON. W. 0. HODGKINSON, M.L.A., F.R.GS., 
 
 Minister for Mines and Public Instruction, Queensland. 
 
 
 
 
 
 BRISBANE: 
 JAMES CHARLES BEAL, GOVERNMENT PRINTER, WILLIAM STREET. 
 
 LONDON : 
 DULAU AND CO., 37, SOHO SQUARE, 
 
 1892. 
 
DMevicated 
 
 TO THE MEMORY OF THREE WORTHY PIONEERS IN AUSTRALIAN GEOLOGY, 
 
 SAMUEL STUTCHBURY, 
 
 WILLIAM BRANWHITE CLARKE, 
 
 AND 
 
 RICHARD DAINTREE. 
 

 

 
 PREFACE. 
 
 + : 
 
 GEOLOGY. 
 
 THe material for the present Work has been accumulating ever since my arrival in the 
 Colony in 1877. It was, however, only in the year 1881 that the idea occurred to Mr. R. 
 Etheridge, Junr., and myself to combine our labours, so that in laying a foundation for 
 future work Stratigraphy and Paleontology should go hand in hand.* The necessity for 
 a Handbook explanatory of the Exhibits at the Colonial and Indian Exhibition of 1886 
 brought forth a hastily-written réswmé of the conclusions arrived at up to that date, 
 which must be understood to be superseded by the present volumes. 
 
 But for the encouragement and assistance rendered to me by my Colleague, I 
 question if I should ever have finished my portion of the congenial task. I do not, of 
 course, refer to my work as finished in the sense that nothing need be added to it by 
 myself or others, but it was necessary, at some time or other, to gather together the 
 scattered material which had accumulated, and to regard the collection as a record of 
 the Geology of Queensland up to date. My labours in the field, occupying, as they did, 
 often the greater part of the year, and necessary office and laboratory duties at head- 
 quarters, retarded the progress of the work from year to year. Another cause of delay, 
 and that the most serious, was the difficulty of what is called in legal phraseology 
 “closing the record,” as fresh material poured in from day to day, and called for the 
 reconsideration of many of the results already arrived at. My lifetime, just as well as 
 a portion of it, might have been spent on the work if this difficulty had not been 
 resolutely looked in the face. 
 
 To numerous Writers and many Personal Friends my obligations for assistance 
 rendered are deep and heartfelt. Their services will be found referred to throughout 
 the Work. 
 
 The highest function of a Geological Survey is to lay a basis for future scientific 
 observations by accurately mapping the relations of the various formations met with in 
 a given district. I cannot say that this beau ideal has been reached in Queensland. 
 In every country, and especially in every new country, it becomes necessary in the 
 first place to give attention to districts remarkable for the presence or prospects of 
 mineral deposits. The “Reports” of the Geological Surveys of Queensland form, for 
 the most part, a series of such observations, and include as much stratigraphical work 
 as has been been found possible under the circumstances. By piecing together these 
 isolated surveys, and adding to them such information as is procurabie from outside 
 
 
 
 * We began by publishing conjointly a ‘‘Catalogue of Works, Papers, Reports, and Maps on the 
 Geology, Paleontology, Mineralogy, Mining and Metallurgy, &c., of the Australian Continent and 
 Tasmania.” Svo. London: Stanford: 1881. The Catalogue was republished in 1882 by the New South 
 
 Wales Government, 
 
Vi. PREFACE. 
 
 sources, a Geological Map of the Colony has been compiled with some approach to 
 accuracy, although in many cases all that could be ascertained was that a certain deposit 
 occupied a given position, the boundaries having to be guessed at from the compiler’s 
 knowledge, whether at first or second hand, of the topography of the district in question. 
 
 The first Geological Map of the Colony was a Sketch on the scale of about a 
 hundred miles to the inch issued with the late Mr. Richard Daintree’s Paper “ On the 
 Geology of Queensland,” read before the Geological Society of London on 24th April, 
 1872. The next was a hand-coloured Map on the scale of sixteen miles to an inch, 
 prepared by me for the Colonial and Indian Exhibition of 1886, and which was published 
 in the same year under the authority of the Department of Works and Mines on the 
 reduced scale of thirty-two miles to an inch. The third is that on the scale of sixteen 
 miles to an inch, issued with the present Work. 
 
 As this Work is, to a large extent, based on official Geological Surveys, it may 
 be wel! in this place to give a brief account of the personnel anda list of the publications 
 of these Surveys. 
 
 Prior to the separation of Queensland from New South Wales, the late Rey. 
 W.B. Clarke, F.R.S., &c., was employed by the Government of New South Wales in the 
 Northern District of that Colony, as it now stands, and extended his observations into 
 the Darling Downs and Moreton Bay Districts, which are now included in Queensland. 
 Ina letter, dated 14th October, 1853, addressed to the Colonial Secretary of New South 
 Wales,* Mr. Clarke described the Condamine Basin and the Creeks of the Darling 
 Downs, with their included Marsupial and other remains, the trappean rocks of the 
 Upper Condamine, the auriferous alluvial deposits of Lord John’s Swamp, the slaty 
 rocks of Pikedale, and the portion of the Coalfield on the Condamine Waters. 
 
 Mr. Samuel Stutchbury, F.G.S., Curator of the Bristol Philosophical Institution, 
 on the recommendation of Sir Henry De la Peche, was appointed Geologist for the 
 Colony of New South Wales on 27th December, 1850. Sir Henry described Mr. 
 Stutchbury as “ highly qualified for the service, and well instructed in our mode of 
 work on the Geological Survey of Great Britain.” Mr. Stutchbury held the appoint- 
 ment till the end of 1855, and from October, 1853, was employed chiefly in the Southern 
 portions of what is now Queensland, having extended his observations northward to 
 Keppel Bay, when the state of his health obliged him to resign and return to England. 
 
 Mr. Stutchbury’s Reports were issued tri-monthly, and published as Legislative 
 Assembly Papers. The first to deal with a portion of Queensland is the Tenth, of 
 which I have never seen a copy. It appears to have been descriptive of “ The Eastern 
 Ranges opposite the Berrigal Station.”’ 
 
 The Eleventh Report, dated from the’ Darling Downs, 1st October, 1853, deals 
 with the same neighbourhood, and portions of the Dividing Range between Queensland 
 and New South Wales, and is accompanied by a Geological Map of the district between 
 the Nandawar Range in New South Wales and Talgai in Queensland. 
 
 
 
 * Legislative Assembly Papers, N.S. Wales, fep., 1853. 
 
PREFACE. vil. 
 
 The Twelfth Report is dated from South Brisbane, lst January, 1854, and 
 describes the basalts of the Condamine River and its tributaries, and the portion of the 
 Ipswich Coal Field extending from the Basaltie Range of Toowoomba to Brisbane, and is 
 accompanied by a Geological Map of the district between Dalby and the mouth of the 
 Brisbane River. 
 
 The Thirteenth Report is dated from the Pine River, 20th May, 1854, and is 
 descriptive of the Ipswich Coal Measures. It is accompanied by a Geological Map of 
 the District from Ipswich down the Brisbane River and northward to Caloundra Point, 
 and another showing the Coal crops of the Rivers Brisbane and Bremer. 
 
 The Fourteenth Report dates from Durundur, Ist August, 1854, and describes 
 the Country from the North Pine River, vid Caboolture, to Durundur. In this Report 
 Mr. Stutchbury sums up his observations on the portion of the Ipswich Coal Field 
 visited by him, and it is evident that he had not grasped the idea that it was separable 
 from the Permo-Carboniferous Coal Measures of New South Wales proper. 
 
 The Fifteenth Report, dated from Auckland Creek, near Gladstone, in January, 
 1855, deals with the Country from Colinton to Gladstone, and is accompanied by a 
 Geological Map extending from the junction of the Brisbane and Stanley Rivers to the 
 mouth of the Boyne River. 
 
 Mr. Stutchbury’s Sixteenth and last Report is dated from Sydney, 20th 
 November, 1855, and describes part of the Coast District between the Boyne and 
 Fitzroy Rivers, and is accompanied by a Geological Map. 
 
 Mr. Stutchbury’s Reports display keen powers of observation, and are not known 
 so well as they ought to be. They are, however, extremely difficult to obtain. 
 
 In 1868 Mr. D’Oyley H. Aplin was appointed Geologist for the Southern 
 District of the new Colony of Queensland, and in the same year Mr. Richard Daintree, 
 C.M.G., both formerly of the Geological Survey of Victoria, was appointed Geologist 
 for the Northern District. Mr. Aplin held the appointment till the end of 1869, and 
 Mr. Daintree to the end of 1871. 
 
 Mr. Aplin’s Reports aré seven in number, all in fep., the first two, or perhaps 
 three, published as Legislative Council, and the remainder as Legislative Assembly 
 Papers. 
 
 His First Report, ‘On the Geological and Mining Features of the Gympie 
 Gold Field,” is dated 2nd July, 1868. 
 
 The Second is a Report, dated 10th August, 1868, which I have never been able 
 to obtain. 
 
 The Third, dated 23rd October, 1868, is a ‘‘ Report of the Government Geologist 
 of the Southern District,’ descriptive of an examination (for Gold) of the Country on 
 the east side of the D’Aguilar Range, and of the Neurum-Neurum and Delaney’s 
 Creeks and adjacent Country, as far as the jurection of “he former with the Stanley 
 River. 
 
viii. PREFACE. 
 
 The Fourth, dated 16th January, 1869, is a “ Concluding Report of the Govern- 
 ment Geologist for the Southern Division, on the examination for Gold of the Country 
 south of the Bunya Bunya Range, between the River Brisbane and the Coast, including 
 some Observations on the Gold Deposits at Jimna and Gooroomjam.” 
 
 The Fifth “ Progress Report of the Government Geologist for South Queens- 
 land” is dated 31st March, 1869, and refers to the Talgai Gold Field. 
 
 The Sixth, a “Report on the Auriferous Country of the Upper Condamine, 
 embracing the Diggings at Talgai, Thane’s Creek, Canal Creek, and Lucky Valley,” is 
 dated 28th July, 1869, and is accompanied by a Geological Map. 
 
 The Seventh and last Report, dated 17th January, 1870, is “ On the Geological 
 and Mineral Features of a part of the Southern and Northern Portions of the Burnett 
 District.” 
 
 Mr. Daintree made six Reports (all published in fep. as Legislative Assembly 
 Papers), as follows :— 
 
 (1.) On the Cape River Diggings, and the latest Mineral Discoveries in Northern 
 Queensland, October, 1868. 
 
 (2.) On Gold Discoveries in the Gilbert Ranges (with Map), dated 7th April, 1868. 
 
 (3.) Progress Report on a Portion of the Rockhampton Mining District, with a 
 Geological Map of Mount Wheeler. 
 (4.) General Report on the Northern District, 2nd February, 1870. 
 
 (5.) On the Ravenswood, Mount Wyatt, and Cape River Gold Fields, &c., dated 
 29th August, 1870. 
 
 (6.) Geology of Queensland as represented at London Exhibition, 1871, 3rd Novem- 
 ber, 1871. 
 
 Mr. Daintree went to London in charge of the Queensland Mineral Exhibits at 
 the 1871 Exhibition, and remained there as A gent-General for the Colony. In addition 
 to the above Reports, Mr. Daintree wrote an important Paper, “‘ Notes on the Geology 
 of Queensland,” in the Quarterly Journal of the Geological Society of London, for 
 1872. To this Paper there were appended Descriptions of the Fossils, by Mr. Robert 
 Etheridge, F.R.S., F.G.S., Paleontologist to the Geological Survey of Great Britain, 
 and Mr. W. Carruthers, F'.R.S., F.G.8., Keeper of the Botanical Department in the 
 British Museum. The Geological Map, which has already been referred to, was issued 
 with this Paper, and was afterwards reproduced in colours by the Queensland Govern- 
 
 ment. 
 
 A. Map of Queensland, ‘“ Showing Mineral Areas,” by Mr. Daintree, was issued 
 with a “ Handbook for the Use of Intending Immigrants’’ (n.d.), and again with a 
 smaller ‘* Handbook for Immigrants to Queensland,” London, 1875. Both Ilandbooks 
 were compiled by Mr. Daintree. The first-mentioned contains numerous photographs 
 by him, which are evidently reductions of the large coloured photographs, mostly taken 
 with a view to the illustration of geological structure, which adorned the Queensland 
 Court of the 1871 Exhibition. 
 
PREFACE. ° ix. 
 
 Mr. (now the Hon.) A. C. Gregory, C.M.G., F.R.G.S., formerly Surveyor- 
 General, whose explorations had already added so much to our knowledge of the interior 
 of Australia, held the appointment of Geologist for the Southern District from 1875 
 to 1879. During this period he issued the following Reports (all in fep.) :— 
 
 (1.) On the Geology of Part of the Districts of Wide Bay and Burnett, 19th August, 
 1875. (Legislative Assembly Paper.) 
 
 (2.) On the Coal Deposits of the West Moreton and Darling Downs Districts, 8th 
 March, 1876. (Council and Assembly Paper.) 
 
 (3.) On the Burrum Coal Mines, 9th November, 1878. (By Authority.) 
 
 (4.) Geological Features of the,South-Eastern Districts of the Colony of Queensland, 
 15th September, 1879. (Legislative Assembly Paper.) With reference to this 
 Report, a “ Geological Map of Moreton and Darling Downs,” on the scale of 
 eight miles to an inch, was published by the Government in 1879. 
 
 (5.) On the Search for Coal between Dalby and Roma, 10th September, 1879. 
 (Legislative Assembly Paper.) 
 
 In addition to the above, Mr. Gregory, when Surveyor-General, made a Report 
 “On the Mineral Discoveries on the Head of the Severn River and its Tributaries,” 
 dated 29th April, 1872. (Council and Assembly Paper.) 
 
 After an experieffte of ten years on the Geological Survey of Scotland, I was 
 appointed Geologist for Northern Queensland on 29th March, 1876, and arrived in 
 the Colony in 1877. On Mr. Gregory’s retirement the Geological Survey of the 
 whole Colony was placed under my charge. In 1883, Mr. William H. Rands, 
 A.R.S.M., F.G.S., and on 6th December, 1888, Mr. Andrew Gibb Maitland, F,G.S., 
 who had been trained in England for the Geological Survey, were appointed Assistant 
 Geologists. These gentlemen and myself at present form the Field Staff of the Geological 
 Survey. We have published the following Reports :— 
 
 (1.) On the Geology and Mineral Resources of the District between Charters Towers 
 Gold Field and the Coast, 14th May, 1878.(1879). R.L.J.* Fep. (C. A. Paper). 
 With two Geological Maps. 
 
 (2.) Geological Features of Part of the Coast Range between the Dalrymple and 
 Charters Towers Roads, 7th June, 1878 (1879). R.LJ. Fep. (C. A. Paper). 
 
 (3.) Preliminary Report on the Bowen River Coal Field, 18th July, 1878 (1879). 
 R.L.J. Fep. (C. A. Paper). With a Geological Sketch Map. 
 
 (4.) On the Bowen River Coal Field, 23rd November, 1878 (1879). R.L.J. Fep. (C.A. 
 Paper). With a Geological Sketch Map. 
 
 (5.) On the Normanby and Marengo Gold Fields, 15th May, 1879. R.LJ. Fep. 
 (C. A. Paper). With two Geological Maps. 
 
 (6.) On the Progress of the Search for Coal in the Cook District, 19th June, 1879. 
 R.LJ. Fep. (C. A. Paper). 
 
 (7.) Second Report on the Progress of the Search for Coal in the Cook District, 12th 
 August, 1879. R.LJ. Fep. (C.A. Paper). 
 
 (8.) Explorations in Cape York Peninsula, 1879-80 (1881). R.L.J. Fep. (C. A. Paper). 
 
 (9.) Further Reports on the Progress of the Gold Prospecting Expedition in Cape 
 York Peninsula, 16th February, 1880; and Report on the Wild River Tin Mines, 
 27th October, 1880 (1881). R.L.J. Fep. (C.A. Paper). With a Geological 
 Map. 
 
 
 
 * Robert L. Jack. ’ 
 
PREFACE. 
 
 (10.) Six Reports on the Geological Features of Part of the District to be traversed 
 by the Proposed Transcontinental Railway, 12th October, 1881—1st March, 1882 
 (1885). R.LJ. Fep. (C. A. Paper). With three Geological Maps. 
 
 (11.) On the Little River Coal Field, near Cooktown, 8th May, 1882. R.L.J. Fep. 
 (C. A. Paper). With a Geological Map. 
 
 (12.) On the Stanthorpe Tin Mining District, 24th July, 1882. R.LJ. Fep. (C.A. 
 Paper). ° 
 
 (13.) On the Tin Mines of Herberton, Western, and Thompson’s Creek Districts, and 
 the Silver Mines of the Dry River, 12th May 1883. R.LJ. Fep. (C.A. 
 Paper). With two Geological Maps and six Plates of Sections. 
 
 (14.) First Sketch of a Geological Map of the Hodgkinson Gold Field. R.LJ. 1883. 
 
 (15.) Progress Report of the Government Geologist for the Year 1883. R.L.J., in 
 Annual Report of the Department of Mines for 1883 (1884), p. 54. 
 
 (16.) On the Hodgkinson Gold Field, 7th August, 1884. R.LJ. Fep. (C..A. Paper). 
 With two Geological Maps and five Plates of Sections. 
 
 (17.) On the Mount Morgan Gold Deposits, 8th November, 1884. R.L.J. Fep. 
 (Legislative Assembly Paper). With Geological Map and Sketch Map. 
 
 (18.) On the Gold Deposits of Mount Leyshon, 6th February, 1885. R.LJ. Fep. 
 (C. A. Paper). With a Geological Map. 
 
 (19.) Progress Report of the Government Geologist for the year 1884. R.L.J., in 
 Annual Report of the Department of Mines for 1884 (1885), p. 50. 
 
 (20.) Progress Report of the Assistant Government Geologist for the year 1884. 
 W.H.R.,* in Annual Report of the Department of Mines for 1884 (1885), 
 p. 52. 
 
 (21.) On the Gold Fields of Raglan, Calliope, Milton (Norton), and Cania, in the Port 
 Curtis District, and on the Mineral Deposits in the Burnett District. W.H.R. 
 Fep. (C. A. Paper), 1885. With three Geological Maps and two Plates of 
 Sections. 
 
 (22.) Progress Report of the Government Geologist for the year 1885. R.L.J., in 
 Annual Report of the Department of Mines for 1885 (1886), p. 53. 
 
 (23.) Progress Report of the Assistant Government Geologist for the Year 1885. 
 W.H.R., in Annual Report of the Department of Mines for 1885 (1886), p. 62. 
 
 (24.) On the Burrum Coal Field. W.H.R. Fep. (C.A. Paper), 1886. With two 
 Geological Maps and three Plates of Sections. 
 
 (25.) On the Gold and Silver Deposits in the neighbourhood of Mount Shamrock. 
 W.H.R. Fep. (C. A. Paper), 1886. 
 
 (26.) On the Argentine (Star) Silver Mines, Kennedy District. R.LJ. Fep. (C.A. 
 Paper), 19th October, 1886. With a Geological Map and one Plate of 
 Sections. 
 
 (27.) On the Geology and Mineral Deposits of the country in the vicinity of Clermont. 
 W.H.R. Fep. (C.A. Paper), 1886. With Geological Map and Plate of 
 Sections. 
 
 (28.) On the Geology and Mineral Resources of the Districts of Kilkivan and Black 
 Snake. W.H.R. Fep. (C. A. Paper), 1886. With three Geological Maps and 
 one Plate of Sections. 
 
 (29.) On the Gold Deposits in the neighbourhood of Nanango. W.H.R. Fep.(C.A. 
 Paper), 1886. With Geological Map and two Plates of Sections. 
 
 (30.) Geological Map of Queensland, on the scale of 32 miles to an inch. R.L.J. 
 
 Issued under the authority of the Department of Publie Works and Mines, 
 1886. 
 
 
 
 * William H. Rands. 
 
PREFACE. xi. 
 
 (31.) Handbook of Queensland Geology. R.LJ. 8vo., Brisbane: Warwick and 
 Sapsford, 1886. Also issued with Essays prepared by the authority of the 
 Executive Commissioners in Queensland for the Colonial and Indian Exhibition, 
 London, 1886. 
 
 (32.) Annual Report of the Government Geologist for the year 1886. RL.J., in 
 Annual Report of the Department of Mines for 1886 (1887), p. 63. 
 
 (33.) Annual Report of the Assistant Government Geologist for the year 1886. 
 W.H.R., in Annual Report of the Department of Mines for 1886 (1887), p. 65. 
 
 (34.) Geological Map of the City of Brisbane and its Environs, accompanied by a 
 Report. W.HR. Fep. (C. A. Paper), 3rd February, 1887. 
 
 (35.) Geological Observations in the North of Queensland, 1886-7. R.L.J. Fep. 
 (C. A. Paper), 13th April, 1887. With three Geological Maps. 
 
 (36.) Geology of and Mineral Deposits occurring in the country in the neighbourhood 
 of Beenleigh and of the Logan and Albert Rivers. W.H.R. Fep. (C. A. Paper), 
 12th May, 1887. 
 
 (37.) On Mineral Lease 276, Watsonville. R.L.J. Fep. (Legislative Assembly Paper), 
 
 . 14th May, 1887. With a Geological Map. 
 
 (38.) Report on a Cobalt Lode at Black Snake, Kilkivan. W.H.R. Fep. (C.A. 
 Paper), 1887. 
 
 (39.) On the Geological Features of the Mackay District. R.LJ. Fep. (C.A. 
 Paper), 8th November, 1887. With three Geological Maps. 
 
 (40.) Report on Glenelg and other Reefs in the neighbourhood of Thane’s Creek and 
 Talgai, and certain Mineral Deposits near Stanthorpe. W.H.R. Fep. (C.A. 
 Paper), 14th May, 1887. 
 
 (41.) Annual Progress Report of the Government Geologist for the year 1887. R.L.J., 
 in Annual Report of the Department of Mines for 1887 (1888), p. 81. 
 
 (42.) Annual Progress Report of the Assistant Government Geologist for the year 
 1887. W.H.R., in Annual Report of the Department of Mines for 1887 (1888), 
 p. 92. 
 
 (43.) On the Eidsvold Gold Field. W.H.R, Fep. (C. A. Paper), 1887. With 
 Geological Map and Plate of Sections. 
 
 (44.) Coal Discoveries on the Flinders. R.LJ. Fep. (C. A. Paper), 23rd January, 
 1888. 
 
 (45.) Geology of the Russell River. R.LJ. Fep. (C. A. Paper), 17th March, 1888. 
 With Geological Map. : 
 
 (46.) On Limestone District, part of the Palmer Gold Field. R.LJ. Fep. (C.A. 
 Paper), 18th April, 1888. With a Map. 
 
 (47.) Second Report on the Mount Morgan Gold Deposits. R.LJ. Fep. (C.A. 
 Paper), 12th December, 1888 (1889). With two Plates of Diagrams and Sections. 
 
 (48.) The Mineral Wealth of Queensland. R.LJ. 8vo., Brisbane: Warwick and 
 Sapsford, 1888. With Map showing the positions of Mineral Fields. Issued for 
 the Queensland Commission, Centennial International Exhibition, Melbourne, 
 1888. 
 
 (49.) Annual Progress Report of the Geological Survey for the year 1888 (1889). 
 Eep. (C. A. Paper). 
 
 (50.) On Taranganba Gold Mine. R.L.J. Fep. (C. A. Paper), 18th May, 1889. 
 
 (51.) On the Albert and Logan District. W.H.R. Fep. (C. A. Paper), 1889. With 
 Geological Map and Sheet of Sections. 
 
 (52.) On Gympie Gold Field. W.H.R. Fep. (C. A. Paper), 1889. With two 
 Geological Maps and seven Plates of Sections. 
 
 (53.) Geological Features and Mineral Resources of the Mackay District. A.G.M.* 
 Fep. (C. A. Paper), 1889. With Geological Map and four Plates of Sections. 
 
 
 
 * A, Gibb Maitland. 
 
xi. 
 
 PREFACE. 
 
 (54.) Geological Observations at the heads of the Isaacs, the Suttor, and the Bowen 
 Rivers. A.G.M. Fep. (C. A. Paper), 1889. With three Geological Maps. 
 
 55.) Report on Geological Specimens from New Guinea. R.L.J. and A. W. Clarke. 
 Fep. New Guinea Government Gazette, 5th June, 1889. 
 
 (56.) Report on Geological Specimens from New Guinea. W.H.R. Fep. Dew 
 Guinea Government Gazette, 15th August, 1889. 
 
 (57.) On the Sellheim Silver Mines and surrounding District. R.LJ. Fep. (C. A. 
 Paper), 11th September, 1889. With two Geological Maps and Plate of 
 Sections. 
 
 (58.) Annual Progress Report of the Geological Survey for the year 1889 (1890). 
 With Geological Map. 
 
 59.) The Coal Measures, Neardie Antimony Mine and Teebar and Culgoa Copper 
 Lodes. W.H.R. Fep. (C. A. Paper), 1890. With Geological Map and Plate 
 of Sections. 
 
 (60.) On Mount Biggenden Bismuth Mine, Gebangle, and the Mount Shamrock Mine. 
 W.H.LR. Fep. (C. A. Paper), 1890. With a Geological Map and Plate of Sections. 
 
 (61.) Proposed Boring for Artesian Water on the Etheridge and Croydon Gold Fields. 
 R.L.J. Fep. (C. A. Paper), 18th January, 1890. 
 
 (62.) Proposal to Bore for Artesian Water at Normanton. R.LJ.and A.G.M. Fep. 
 (C. A. Paper), 20th January, 1890. 
 
 (63.) Brookfield, Pullen Vale, and Moggill Districts. W.H.R. Fep. (C.A. 
 Paper), 1890. 
 
 (64.) Coal in the Parish of Noosa. W.H.R. Fep. (C.A. Paper), 29th November, 
 1890. 
 
 (65.) Proposed Boring for Water at Brisbane. R.L.J. Fep. (C. A. Paper), 5th March, 
 1889 (1890). 
 
 (66.) The Tin Mines near Cooktown. R.L.J. Fep. (C. A. Paper), 6th December, 1890 
 (1891). With Geological Map and two Sheets of Plans. 
 
 (67.) The Mineral Selections on the Ballandean and Jibbinbar Runs. W.H.R. Fep. 
 (C. A. Paper), 1890. 
 
 (68.) The Paradise Gold Field. W.H.R. Fep. (C.A. Paper), 1891. 
 
 (69.) The Chillagoe and Koorboora Mining Districts. R.LJ. Fep. (C. A. Paper), 
 6th November, 1890 (1891). With Map and Geological Map. 
 
 (70.) The Geology of the Cooktown District. A.G.M. Fep. (C. A. Paper), 1891. 
 With Geological Map and two Sheets of Sections. 
 
 (71.) Geology and Mineral Resources of the Upper Burdekin. A.G.M. Fep. (C. A. 
 Paper), 1891. With Geological Map and two Sheets of Sections. 
 
 (72.) The Coolgarra Tin Mines and Surrounding District. A.G.M. Fep. (C.A. 
 Paper), 1891. With Geological Map and Sheet of Plans. 
 
 (73.) The Cape River Gold Field. W.H.R. Fep. (C.A. Paper), 1891. With two 
 Geological Maps and two Plates of Sections. 
 
 (74.) Notes on Broken Hill (N.S.W.) R.L.J. Fep. (C. A. Paper), 15th May, 1891. 
 (75.) Geology of Magnetic Island. A.G.M. Fep. (C. A. Paper), 1892. 
 (76.) Second Report on Gympie Gold Field. W.H.R. Fep. (C. A. Paper), 1891. * 
 
 (77.) Annual Progress Report of the Geological Survey for the year 1890. With 
 Plate of Sections, and Geological Maps of Cania and part of Gilbert Gold Fields. 
 Fep. (C. A. Paper), 1891. 
 
 (78.) Report on Moondilla Gold Field. R.L.J. Fep. (C. A. Paper), 1891. 
 
 (79.) Report on an Alluvial Cinnabar Deposit near Kilkivan. W.H.R. Fep. (C. A. 
 Paper), 1892. 
 
PREFACE. xiii. 
 
 (80.) Report on the New Discovery of Coal near the Callide Creck, Port Curtis 
 District. W.H.R. Fep. (C. A. Paper), 1891. 
 
 (81.) Report on Sapphire Deposits and Gold and Silver Mines near Withersfield. 
 R.L.J. Fep. (C. A. Paper), 1892. With a Map. 
 
 (82.) Report on the Kangaroo Hills Silver and Tin Mines. R.LJ.  Fep. (C. A. 
 Paper), 1892. With a Geological Map. 
 
 (83.) Third Report on the Mount Morgan Gold Deposits. R.L.J. Fep. (C. A. Paper), 
 1892. With Maps, Views, and Sections. 
 
 (84.) Report on the Styx River Coal Field. W.H.R. Fep. (C. A. Paper), 1892. 
 With Geological Map. 
 
 (85.) Geological Observations in British New Guinea in 1891. A.G.M.  Fep. (C. A. 
 Paper), 1892. With Geological Maps and Sections. 
 
 (86.) Report on Olsen’s and Johannsen’s Caves, near Rockhampton. W.H.R. Fep. 
 (C. A. Paper), 1892. With Map and Plate. : 
 
 (87.) Report on Supposed Gold-bearing Quartzites, near Traveston and Glastonbury ; 
 and on Hyalite in Basalt, near Cooran. W.H.R. Fep. (C. A. Paper), 1892. 
 
 (88.) Annual Progress Report of the Geological Survey for the Year 1891. Fep. 
 (C. A. Paper), 1892. 
 
 From February, 1889, to his death, on 10th April, 1891, Mr. James Smith was 
 employed as Collector for the Survey. Mr. Smith had for many years previously been 
 collecting fossils and other Natural History specimens, many of which he donated to the 
 Geological Survey. His appointment to the staff of the Survey enriched the collections 
 with representative fossils from Rockhampton, Langmorn, Raglan, Broadsound, Bar- 
 cealdine, the Drummond Range, and the Ipswich Coal Field. Mr. Smith, who was an 
 enthusiastic naturalist, wrote a Paper “On the Discovery of Fossils at Rock- 
 hampton,’* and contributed numerous articles to the Natural History Society of Rock- 
 hampton and the Rockhampton Bulletin. His place on the Survey will be very difficult 
 to fill. 
 
 Mr. William Wood acted as Caretaker to the Survey Museum from 28th May, 
 1886, to 3lst May, 1891, when he retired, owing to the failure of his health. His place 
 is now filled by Mr. Thomas Sythers. 
 
 My Colleague, Mr. Robert Etheridge, Junr., has acted as Consulting Paleon- 
 tologist in an honorary capacity ever since my arrival in Queensland. His connection 
 with the British Museum, the Australian Museum, and the Geological Survey of New 
 South Wales, and his former connection with the Geological Surveys of Victoria and 
 Scotland, rendered him peculiarly fitted for this task. To my association with him in 
 Scotland, I owe a friendship which has been very valuable to me as well as to the Colony 
 of Queensland. The magnitude of Mr. Etheridge’s labours on our behalf may be esti- 
 mated by his contribution to the present work. 
 
 For some time back I have urged on the Government the attachment of a 
 Chemist to the staff of the Survey. The three working members of the staff are 
 chiefly employed, and can always be most profitably employed in the field, and have 
 little time to devote to micro-petrographical work or to the chemical questions which 
 arise in the course of their observations. I am, however, enabled through the kindness 
 
 ee Ea ec en a a ee Dee 
 * Proc. Austr, Assoc. Adv. Sci., 1888, vol. i., p. 300. 
 
xiv. PREFACE. 
 
 of my friend Mr. A. W. Clarke, F.G.S., of Charters Towers, formerly Government 
 Mineralogical Lecturer, to furnish an extensive series of Petrographical Notes on 
 
 Queensland Rocks, the result of at least two years’ assiduous labour. 
 
 It was originally my intention to include in the present volume all that I could 
 say regarding the Mines of the Colony, but I had not made great progress when I 
 became convinced that this would not only lengthen the work beyond all reasonable 
 limits, but would also be a source of further delay. Notes will be found in the 
 following pages on most of the Mining Districts, and I have drawn freely for statistics, 
 &e., on “The Mineral Wealth of Queensland,”’* taking care, however, to bring the 
 information up to date where it was possible; but the Economic Geology of Queensland 
 must form the subject of another volume. I am informed that The Honourable 
 W. O. Hodgkinson, Minister for Mines and Education, has a Work on this subject in 
 preparation.t 
 
 ROBERT L. JACK. 
 Brisbane, 8th August, 1892. 
 
 PALZONTOLOGY. 
 
 The investigation of the material for the Paleontology of Queensland and New 
 Guinea was commenced in 1881, and has progressed at intervals since that date as 
 opportunity would permit during the leisure time of the Writer. 
 
 The Paleontology of Queensland has hitherto been treated only in a disjointed 
 and desultory manner, whilst that of New Guinea, to all intents and purposes, is 
 untouched and hardly known. The present attempt is the first on which a collective 
 account of the Fossil Organic Remains of these countries has appeared. 
 
 Up to 1872 Sir Richard Owen’s masterly descriptions of the large extinct Mar- 
 supialia, a notice by Prof. (now Sir) F. McCoy on some Reptilian Remains, and a few 
 Mollusea, and the more extended essay of the late Mr. Charles Moore on the Mesozoic 
 Fossils of Wollumbilla, were the only Memoirs of any importance extant. In that year 
 there appeared an account of the gatherings of the late Richard Daintree, C.M.G., by 
 Messrs. Etheridge and Carruthers. Since then large collections have been made, chiefly 
 through the labours of my Colleague, Mr. R. L. Jack, his Assistants, Mr. W. H. Rands 
 and Mr. A. Gibb Maitland, and by the late Mr. James Smith, of Rockhampton, frst as 
 a private individual and afterwards as Collector for the Geological Survey. In addition 
 many separate Papers have appeared, notably “Carboniferous Marine Fossils,” 
 “Mesozoic Fossils from the Palmer River,” and “ Fossil Flora of the Coal Deposits of 
 
 
 
 * See No, 48 in the preceding list of Publications. 
 
 + Throughout the Work the paragraphs written by my Colleague and myself are distinguished by an 
 initial (E. or J.) at the end. 
 
 { With the exception of a short Paper by the Writer, ‘‘On our Present Knowledge of the Paleon- 
 tology of New Guinea,” in Records of the Geological Survey of New South Wales, vol. ii., p. 172. Sydney; 
 Government Printer ; 1890, 
 
PREFACE. xv. 
 
 Australia,” by the late Rey. J. E. Tenison Woods; Dr. O. Feistmantel, “ Palaeozoische 
 und Mesgozoische Flora” ; the ‘ Paleozoic Corals of North Queensland,” by Prof. H. A. 
 Nicholson and the Writer; the ‘“ Fossils of the Bowen River Coal Field,” by the 
 Writer; and others of minor importance. 
 
 The work may be divided into two parts, the first treating of the Paleontology 
 of Queensland ; the second recording what little is known of that of New Guinea. In 
 describing the Queensland Organic Remains, I have grouped them in very general 
 and broad geological sections, consequent on the present tentative grouping of the 
 sedimentary deposits. The general determination of the species has been rendered 
 more difficult than ordinary by the poor state of preservation of a large number of the 
 specimens. This will, to a great extent, explain the number of species simply indicated 
 (sp. ind.) and not named, as I thought it better to figure such when possessing any 
 marked character, with the view of future determinate recognition. The species 
 described represent not only those which have come under the eye of the Writer, but 
 others published by various Authors, chiefly in the ‘Annals and Magazine of Natural 
 History” and the “ Quarterly Journal of the Geological Society of London.” In many 
 cases descriptions are quoted verbatim, with the kind permission of Dr. Francis on the 
 one hand, and the leave of the Council of the Geological Society on the other. In such 
 cases the Author’s name is invariably given at the end of the extract in brackets. Similarly 
 lengthy extracts have been made from a Paper of my own in the “ Proceedings of the 
 Royal Physical Society of Edinburgh,” again with the kind permission of the Council. 
 
 I have endeavoured to arrange the subject matters under each species in the 
 clearest possible manner. Following the name of the fossil will usually be found a 
 brief synonymy, detailing only the principal works in which previous allusions to it will 
 be found. To the synonymy succeeds the specific description when it has been found 
 requisite to give one, otherwise general observations follow next, and the account is 
 completed by the locality and horizon. In the synonymy I have endeavoured strictly 
 to adhere to priority in the use of specific names, but I wish it to be distinctly 
 understood that newspaper articles (a medium unfortunately adopted by more than 
 one Australian Writer of note) have been purposely ignored. In the paragraph relating 
 to the locality and horizon, the former is invariably followed by the name of the 
 collector, or recorder, when known to me, and in italics to give it greater prominence ; 
 but when the name of the collector is unknown, that of the describer is substituted. I 
 have also endeavoured, but not always with success I am afraid, to indicate the Collection 
 or Museum containing the specimens mentioned; and the absence of such reference 
 will, in the great majority of instances, infer that the fossils are in that of the Queens. 
 
 land Geological Survey. 
 
 I am indebted to a large number of scientific friends for most cordial assistance. 
 Had it not been for the constant kindness and encouragement of my old Colleague and 
 Co-Author, the many difficulties which crop up in the production of a Work of this kind 
 would probably have proved fatal to it. At no time was this more felt than on its 
 resumption after my arrival in Sydney, when the sad lack of Paleontological literature 
 in the Colonies was forcibly brought home to me. 
 
XVi. PREFACE. 
 
 For assistance in their respective special groups I have to acknowledge my great 
 indebtedness to Profs. H. A. Nicholson, M.D., of Aberdeen; T. Rupert Jones, F.RS., 
 of London; Ralph Tate, F.L.S., of Adelaide; Sir F. McCoy, F.R.S., of Melbourne ; 
 T. W. Edgeworth David, B.A., Sydney; the late Dr. P. H. Carpenter, F.R.S., of Eton, 
 and the late Dr. T. Davidson, F.R.S., of Brighton (Eng.); Messrs. Edgar Smith, of the 
 British Museum; Stuart Ridley, late of the same Institution; and John Brazier, 
 O.M.Z.8S.; George Sweet, Melbourne; and T. Whitelegge, of the Australian Museum. 
 
 For general assistance and advice I am equally beholden to Mr. R. Etheridge, 
 F.RS., and Dr. Henry Woodward, F.R.S., of the British Museum. 
 
 Dr. G. J. Hinde, of Mitcham (Eng.), has most kindly conducted an original 
 investigation of the interesting Cretaceous Sponge, Purisiphonia Clarkei, for these 
 pages; and I am thus able to afford a much more detailed account of this species. 
 
 But to none am I more indebted than to Messrs. Robert Kidston, of Stirling, 
 N.B., and R. B. Newton, of the British Museum. The former conducted the exami- 
 nation of the Paleozoic and Mesozoic Plants, and drew up a lengthy series of notes, 
 which have proved of the greatest assistance. After my departure from London, Mr. 
 Newton undertook the task of superintending the drawing of the lithographic plates, 
 and general custody of the figured specimens. ‘This, no light duty, has greatly 
 contributed to the completion of this undertaking. 
 
 The success of all works on Paleontology depends in a great measure on the 
 illustrations; and I was fortunate in securing the careful and well-known artistic skill 
 of my friends, Messrs. Charles Berjeau and Percy Highley. Taking into consideration 
 the exceptional circumstances under which the plates were drawn, they reflect the 
 greatest credit on these gentlemen. Additional plates (Nos. 37 to 44 inclusive) have 
 been kindly undertaken by Mr. G. H. Barrow, of the Australian Museum. 
 
 Messrs. Richard Hall and W.H. Brown, the former of, the latter late of, the 
 Department of Geology, British Museum, have rendered me very valuable assistance— 
 the one in preparing microscopic sections and developing specimens, the other in helping 
 to unravel many difficult questions of bibliography. 
 
 Finally, as to the sources of the specimens described. The major portion are, 
 of course, the result of the Geological Explorations of my Colleague and his Assistants. 
 In addition to this, a valuable collection from the Rockhampton District was contributed 
 by the late Mr. James Smith, of Rockhampton, who was also most kind in affording 
 general local information. Mr. C. W. De Vis, Curator of the Queensland Museum, 
 forwarded me another large series from the same neighbourhood, and many fine 
 Cretaceous fossils from various localities. Besides these the cabinets of the British 
 Museum, Australian Museum, and the Mining and Geological Museum, Sydney, have 
 been laid under contribution. I am indebted to the Rev. H. H. Winwood, M.A., for 
 the loan of the few existing specimens of the late Rev. W. B. Clarke’s Collection, 
 described by the late Mr. Charles Moore,* now in the Museum of the Philosophical 
 
 
 
 
 
 * Quart. Journ. Geol. Soc., 1870, xxvi., pp. 226-261. With the exception of these specimens, the 
 whole of Mr. Clarke’s Collection was burnt in the Garden Palace fire at Sydney in 1882. 
 
PREFACE. XVll. 
 
 Society of Bath (Eng.) The gatherings of my old Colleague, the late Richard Daintree, 
 described by my Father,* have become much scattered, and it is difficult to refer to 
 their present place of exhibition. The Corals are in the British Museum, and I have 
 received some of the Mollusca from the Queensland Museum, but they do not all appear 
 to be there. I was permitted to borrow a few fossils from the Collection of the late 
 Rey. J. E. T. Woods, and through the courtesy of the late Prof. W. H. Stephens, M.A., 
 access was granted to many of the plants described by Mr. Woods in his Memoir on the 
 “Flora of the Coal Deposits of Australia,”’+ now in the Macleay Museum at, the 
 University of Sydney. 
 
 A Bibliography of the principal Papers relating to the Paleontology of Queens- 
 land is given herewith. 
 
 It may be necessary to point out that as it is now some time since the Plates 
 were printed off, the titles affixed to some of them are not in accord with the classifica- 
 tion finally adopted, and reflect opinions now abandoned as to the age of certain 
 formations. This, however, is of little importance, as the changes adopted will be noted 
 in the text. ; 
 
 ROBERT ETHERIDGE, Junr. 
 Sydney, 10th August, 1892. 
 
 * Quart. Journ. Geol. Soc., 1872, xxviii., pp. 317-350, 
 + Proc, Linn. Soc. N.S. Wales, 1883, viii., pt. 1, pp. 37-167. 
 

 
LIST OF PAPERS, &¢., RELATING TO THE PALEONTOLOGY OF 
 QUEENSLAND AND NEW GUINEA. 
 
 ae 
 
 Baver, G.—The Systematic Position of Meiolania, Owen. Ann. and Mag. Nat. Hist., 
 1889, ili. (6), pp. 54-62. 
 
 Bennett, G.—Notes on the Chlamydosaurus, or Frilled Lizard, of Queensland (C. Kingii, 
 Gray), and the Discovery of a Fossil Species on the Darling Downs, 
 Queensland, Proc. R. Soc. Tas. for 1875, pp. 56-58. 
 
 BovLenesr, G. A.—On the Systematic Position of the Genus Miolania, Owen (Ceratochelys, 
 
 Huxley). Proc. Zool. Soc. for 1887, Pt. 3, p. 554; Ann. and Mag. 
 Nat. Hist., 1889, iii., pp. 138-141. 
 
 Bowrrsayk, J. S.—A Monograph of the Silico-fibrous Sponges. Proc. Zool. Soc., 1869, 
 pp. 323-351. [Purisiphonia Clarkei, Bk. ] 
 
 CarrurHers, W.—Notes on Fossil Plants from Queensland, Australia. Quart. Journ. 
 Geol. Soc., 1872, xxviil., pp. 350-360, pls. 26 and 27. 
 
 Canter, H. J.—Emendatory Description of Purisiphonia Clarket (Bk.), a Hexactinellid 
 Fossil Sponge, from N.W. Australia. Ann. and Mag. Nat. Hist., 
 1878, i., pp. 376-379. 
 
 Crarke, W. B.—On the Genera and Distribution of Plants in the Carboniferous System 
 of New South Wales. Quart. Journ. Geol. Soc., 1848, iv., pp. 60-63. 
 
 Id. On the Relative Positions of certain Plants in the Coal-bearing Beds of 
 Australia. Quart. Journ. Geol. Soc., 1861, xvii., pp. 354-362. 
 
 Id. On the Occurrence of Mesozoic and Permian Faune in Eastern Australia. 
 Quart. Journ. Geol. Soc., 1862, xviil., pp. 244-247. 
 
 Id. On the Age of the New South Wales Coalfields. Ann. and Mag. Nat. Hist., 
 1862, x., pp. 81-86. 
 
 Id. On the Carboniferous and other Geological Relations of the Maranoa 
 
 District in Queensland, in reference to a discovery of Zoological 
 Fossils at Wollumbilla Creek, and Stony Creek, West Maitland. 
 Trans. R. Soc. Vict., 1865, vi., pp. 32-42. 
 
 Id. On Marine Fossiliferous Secondary Formations in Australia. Quart. Journ. 
 Geol. Soc., 1867, xxiii., pp. 7-12. 
 
 Sth Dinornis an Australian Genus. Geol. Mag., 1869, vi., pp. 383, 384. 
 
 Id. On the Dinornis and Saurian Remains in Australia. American Journ. Sct., 
 1870, xlix., p. 273. 
 
 Id. ‘Remarks on the Sedimentary Formations of New South Wales, 1870. 
 
 Sydney, 8vo. (and later Editions). 
 Dartntree, R.—Age of the New South Wales Coal-Beds. Geologist, 1864, vil., pp. 72-79. 
 
 Id. Report onthe Cape River Diggings, and the latest Mineral Discoveries 
 in North Queensland. Pp.7. Fep. Brisbane, 1868. [Discovery of 
 Belemnites. | 
 
 Id. Notes on the Geology of the Colony of Queensland. Quart. Journ. Geol. 
 
 Soc., 1872, xxviil., pp. 271-317. 
 Dawson, J. W.—Note in Vindication of Leptophelum rhombicum and Lepidodendron 
 gaspianum. Quart, Journ. Geol. Soc., 1873, xxix., pp. 369-371; Geol. 
 Magy., 1873, x., p. 234. 
 Id, Notes on New Erian (Devonian) Plants. Quart. Journ. Geol. Soc., 1881, 
 XXXVil., pp. 299-308, pls. 12 and 13. (Dicranophyllum australicum.) 
 
xx. 
 
 LIST OF PAPERS. 
 
 De Vis, OC. W.—On Remains of an Extinct Marsupial [Sthenurus Charon, de Vis]. Proc. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 is 
 
 Id. 
 
 Id. 
 
 Id, 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 
 Id. 
 Id. 
 
 Id. 
 
 Id. 
 
 Jd. 
 
 Linn. Soc. N.S. Wales, 1883, vii., Pt. 1, pp. 11-15. 
 
 On Brachalletes Palmeri, an Extinct Marsupial. Proc. Linn, Soc. 
 N.S. Wales, 1883, viii., Pt. 2, pp. 190-193. 
 
 Notes on a Lower Jaw of Palorchestes Azael. Proc. Linn. Soc. N.S. Wales, ~ 
 1883, viii., Pt. 2, pp. 221-224. 
 
 On a Fossil Calvaria [Chronozoon australe, De Vis]. Proc. Linn. Soe. 
 
 . N.S. Wales, 1883, viii., Pt. 3, pp. 392-395. 
 
 On a Fossil Humerus [Nototherium ? from Darling Downs]. Proc. Linn. Soc. 
 N.S. Wales, 1883, viii., Pt. 3, pp. 404-408. 
 
 The Moa (Dinornis) in Australia. Proc. R. Soc. Queensland, 1884, i., Pt. 1, 
 pp. 23-28, pls. 3 and 4. 
 
 Ceratodus Fosteri, Post Pliocene. Proc. R. Soc. Queensland, 1884, i., Pt. 1, 
 pp. 40-43. 
 
 On Bones and Teeth of a large Extinct Lizard (Notiosaurus dentatus, Owen). 
 Proc. R. Soc. Queensland, 1885, ii., Pt. 1, pp. 25-32, pls. 1-3 
 
 On an Extinet Monotreme, Ornithorhynchus agilis. Proc. R. Soc. Queens- 
 land, 1885, ii., Pt. 1, pp. 35-38, pl. 4. 
 
 On Remains of an Extinct Saurian (Pallimnarchus pollens, de Vis). Proc. 
 R. Soc. Queensland, 1886, ii., Pt. 2, pp. 181-191, pls. 10-15. 
 
 On a supposed New Species of Wototherium. Proc. Linn. Soc. N.S. Wales, 
 1887, ii. (2), Pt. 4, pp. 1065-1070, pl. 38. 
 
 A Post-Pliocene Artiodactyle. Froc. R. Soc. Queensland, 1887, iii., 
 pp. 42-47, pl. 1. 
 
 Ona Femur probably of Thylacoleo. Proc. R. Soc. Queensland, pp. 122-128, _ 
 pls. 3 and 4. : 
 
 On an Extinct Mammal of a Genus apparently new [Owenia, De Vis], 
 Proc. R. Soc. Queensland, 1887, iv., pp, 99-106, pls. 1-4. 
 
 On Diprotodon minor, Hux. Proc. R. Soc. Queensland, 1888, v., Pt. 2, 
 pp. 38-44, plate (upper figs.) 
 
 Note on the Genera Zygomaturus and Nototherium. Proc. R. Soc. Queens- 
 land, 1888, v., Pt. 3, pp. 111-116, plate. 
 
 Australian Ancestry of the Crowned Pigeon of New Guinea. Proc. R. 
 Soc. Queensland, 1888, v., pp. 127-131, plate. 
 
 On a New Genus of Extinct Mammals (Synaptedon). Proc. R. Soc. Queens- 
 land, 1889, v., Pt. 5, pp. 158-160. 
 
 On an Extinct Genus of the Marsupials allied to Hypsiprymnodon. Proc. 
 Linn. Soc. N.S. Wales, 1888, iii. (2), Pt. 1, pp. 5-8, pl. 1. 
 
 A Glimpse of the Post-Tertiary Avi-fauna of Queensland. Proc. Linn. Soc. 
 N.S. Wales, 1888, iii. (2), Pt. 3, pp. 1277-1292, pls. 33-36. 
 
 Additions to the List of Fossil Birds. Proc. R. Soc. Queensland, 1889, vi. 
 Pt. 1, pp. 55-58. 
 
 On Megalania and its Allies. Proc. R. Soc. Queensland, 1889, vi., Pts. 
 2 and 3, pp. 93-99, pl. 4° 
 
 On the Phalangistide of the Post-Tertiary Period in Queensland. Proc. 
 R. Soe. Queensland, 1889, vi., Pts. 2 and 3, pp. 105-114. 
 
 On a Bone of an Extinct Eagle. Proc. R. Soc. Queensland, 1889, vi., Pt. 4, p. 61. 
 
 The Moa in Queensland. NV. Zealand Journ. Sci., 1891, i. (2), No. 3, 
 pp. 97-101. 
 
 On the Trail of an Extinct Bird. Proc. Linn. Soc. N.S. Wales, 1891, vi. 
 (2), Pt. 1, pp. 117-122. 
 
 Note on an Extinct Eagle. Proc. Linn. Soc. N.S. Wales, 1891, vi. (2), Pt. 1, 
 pp. 123-125. 
 
 Residue of the Extinct Birds of Queensland as yet detected. Proc. Linn. 
 Soc. N.S. Wales, 1892, vi. (2), Pt. 3, pp. 437-456, pls. 23 and 24, 
 
LIST OF PAPERS. XXL 
 
 ErHeriver, R.—Description of the Palwozoic and Mesozoic Fossils of Queensland. Quart. 
 Journ. Geol. Soc., 1872, xxviii., pp. 317-350, pls. 13-25. 
 
 Ernerrver, R., Junr.—Notes on some Upper Paleozoic Polyzoa from Queensland. Trans R. 
 Soc. Vict., 1876, xii., pp. 66-68. 
 
 Id. A Catalogue of Australian Fossils, &c., 1878. Cambridge, 8vo. 
 
 Id. On the History of Paleozoic Actinology in Australia. Zrans. R. Soc. 
 Vict., 1878, xiv., pp. 102-108. 
 
 Id. Report on a Collection of Fossils from the Bowen River Coal Field and 
 
 the Limestone of the Fanning River, North Queensland. Proc. R. 
 Phys. Soc. Edinburgh, 1880, v., pp. 263-328, pls. 7-17. 
 
 Id. Further Remarks on Australian Strophalosie ; and Description of a New 
 Species of Aucella from the Cretaceous Rocks of North-east 
 Australia. Journ. R. Soc. N.S. Wales-for 1883 [1884], xvii., pp. 
 87-92, 2 pls. 
 
 Id. [Catalogue of a Collection of Organic Remains representing the 
 Sedimentary Deposits of Queensland.]  Quwzensland Cat. Col. 
 and Indian Exhib., 1886, pp. 152-167. 
 
 Id. Notochelys costata, Owen. Geol. Mag., 1886, iii., p. 239. 
 
 Id. Description of Fish Remains from the Rolling Downs Formation of 
 Northern Queensland. Proc. Zinn. Soc. N.S. Wales, 1888, i, Pt. 
 1, pp. 156-161, pl. 4. 
 
 Id. On Additional Evidence of the genus Ichthyosaurus in the Mesozoic 
 Rocks (Rolling Downs Formation) of North-eastern Australia. 
 Proc. Linn. Soc. N.S. Wales, 1888, ii., Pt. 2, pp. 405-409, pl. 7. 
 
 Id. On Additional Evidence of Plesiosaurus in the Mesozoic Rocks of 
 Queensland. Proc. Linn. Soc. N.S. Wales, 1888, iii., Pt. 2, pp. 
 410-413, pl. 8. 
 
 Id. The Further Discovery of Plesiosaurian Remains in Queensland. Ann. 
 Report Dept. Mines N.S. Wales for 1887 [1888], p. 167. 
 Id. On Further Evidence of a large Struthious Bird (Dromornis, Owen) 
 
 from the Post-Tertiary Deposits of Queensland. Records Geol, 
 Survey, N.S. Wales, 1889, i., Pt. 2, pp. 126-136, pls. 11-13. 
 
 Id. Note on Dromornis australis, Owen. Records Geol. Survey N.S. 
 Wales, 1890, 11., Pt. 1, p. 36. 
 Id. Note on the Occurrence of Fish Remains in the Rocks of the Drummond 
 
 Range, Central Queensland. Records Geol. Survey N.S. Wales, 
 1890, ii., Pt. 2, p. 71. 
 
 Id. On the Occurrence of Microscopic Fungi, allied to the Genus Pa/eachlya, 
 Dunean, in the Permo-Carboniferous Rocks of N.S. Wales and 
 Queensland. Records Geol. Survey N.S. Wales, 1891, 11., Pt. 3, pp. 
 95-99, pl. 7. 
 
 Id. Lepidodendron australe, McCoy. Its Synonyms and Range in Eastern 
 Australia. Records Geol. Survey N.S. Wales, 1891, 11., Pt. 3, pp. 
 119-134. 
 
 Erueripce R., Junr., and Foorp, A. H.—On Two Species of Alveolites, and one of Amplexopora, 
 from the Devonian Rocks of North Queensland. Ann. and Mag. 
 Nat. Hist., 1885, xiv., pp. 175-179, pl. 6. 
 
 Erneriper, R., Junr., and Woopwarp, A. S.—On the Occurrence of the Genus Belonostomus 
 in the Rolling Downs Formation (Cretaceous) of Central Queensland. 
 Trans. R. Soc. Vict., 1891, ii. (2), Pt. 2, pp. 1-6, pl. 1. 
 
 FrEIstMaNnTEL, O.—Palacozischeo und mesozoische Flora des Oestlichen Australiens. 
 Palaeontographica; 1878, Suppl., Bd. iii., Lief. 3, Heften 2-4. 
 
 Id. Notes on the Fossil Flora of Eastern Australia and Tasmania. Geol. Maq., 
 
 1879, vi., pp. 485-492 ; Jowrn R. Soc. N.S. Wales for 1880 [1881], 
 xiv., pp. 103-118. 
 
XXii. LIST OF PAPERS. 
 
 Hinpz, G. J.—Catalogue of the Fossil Sponges in the Geological Department of the British 
 Museum (Natural History) &c. (4to., London, 1883) [ Purisiphonia 
 Clarkei, Bk.) 
 
 Hup.urstron, W. H.—Notes on some Mollusca from South Australia, obtained near Mount 
 Hamilton and the Peak Station. Geol. Mag., 1884, i., pp. 339-342, 
 Pls: 
 
 Id. Further Notes on some Mollusca from South Australia. Geol. Magq., 
 1890, vit. (3), pp. 241-246, pl. 9. 
 
 Hvuxtiry, T.—Preliminary Note on the Fossil Remains of a Chelonian Reptile, Ceratochelys 
 Sthenurus, from Lord Howe’s Island, Australia. Proc. R. Soc., 1887, 
 xlii., pp. 232-238. 
 
 Letcauarpt, L.—Notes on the Geology of Parts of New South Wales and Queensland, made in 
 1842-43 ; translated by G. H. F. Ulrich, Esq., F.G.S., and edited by 
 the Rev. W. B. Clarke, M.A., F.G.8., &e. Waugh’s Almanac, 
 Sydney, 1867-68. 
 
 Ld. Journal of an Overland Expedition in Australia, from Moreton Bay to Port 
 Essington, &e. 8vo. London, 1847. 
 
 LyprxKker, R.—Nototherium and Zygomaturus. Ann. and Mag. Nat. Hist., 1889, iii. (6), 
 
 pp. 149-162. 
 
 lds Catalogue of the Fossil Mammals in the British Museum (Natural History). 
 8vo. London, 1887. 
 
 Id. Catalogue of the Fossil Reptilia and Amphibia in the British Museum 
 (Natural History). Partsi. andi. 8vo. London, 1888-89. 
 
 Td. Catalogue of the Fossil Birds in the British Museum (Natural Besa: 8vo. 
 
 London, 1891. 
 McCoy, F.—Remarks on a Series of Fossils collected at Wollumbilla, and transmitted by Rev. 
 W. B. Clarke, of Sydney. Zrans. R. Soc. Vict., 1865, vi., pp. 42-46. 
 Id. Note on the Cretaceous Deposits of Australia. Ann. and Mag, Nat. Hist., pp. 
 1865, xvi., 333-334. 
 Id. On the Discovery of Cretaceous Fossils in Australia. Trans. R. Soc. Vict., 1866, vii. 
 
 Id. On the Occurrence of Plestosaurus and Ichthyosaurus in Australia. Ann. and 
 Mag. Nat. Hist., 1867, xix., pp. 355-356. 
 ld: On the Discovery of aio cus aaa other Cretaceous Fossils in Australia. 
 
 Trans. R. Soc. Vict., 1868, vili., p. 41. 
 Id. On the Teeth and Fossil Eye of Ichthyosaurus australis. Trans. R. Soc. Vict., 
 1869, Pt. 2, pp. 77-78. 
 Moore, C.—Australian Mesozoic Geology and Palxontology. Quart. Journ. Geol. Soc., 1870, 
 XXVi., pp. 226-261, pls. 10-18. 
 Nicuotson, H. A., and Eruerrpes, R., Junr.—Descriptions of Paleozoic Corals from Northern 
 Queensland, with Observations on the Genus Stenopora. Ann. and 
 Mag. Nat. Hist., 1879, iv., pp. 216-226, 265-285, pl. 14. 
 Td: On the Tasmanian and Australian Species of the Genus Stenopora, Lonsdale. 
 Ann. and Mag. Nat. Hist., 1886, xvii., pp. 173-187, pls. 3 and 4. 
 Owen, R.—Descriptive Catalogue of the Osteological Series contained in the Museum of the 
 Royal College of Surgeons of England. 4to. London, 1850, &c. 
 [Vol. i, Marsupialia. ] 
 Id. On the Discovery of the Remains of a Mastodontoid Pachyderm in Australia. 
 Ann. and Mag. Nat. Hist., 1843, xi., pp. 7-12. 
 Ld. Additional Evidence proving the Australian Pachyderm, &c., to be a Dinotherium, 
 with Remarks on the Nature and Affinities of that Genus. Ana. 
 and Mag. Nat. Hist., 1843, xii., pp. 329-332. 
 Id. Report on the Extinct Mammals of Australia, with Descriptions of certain Fossils 
 indicative of the former existence in that Continent of large 
 Marsupial Representatives of the Order Pachydermata. Brit. 
 Assoc. Report for 1844 [1845], pp. 223-240. 
 
LIST OF PAPERS. Xxiil. 
 
 Owen, R.—On some outline Drawings and Photographs of the Skull of Zygomaturus trilobus 
 
 Id. 
 
 Ia. 
 
 Id. 
 
 Id. 
 Id. 
 
 Id. 
 
 Id. 
 
 Id, 
 Id. 
 Id. 
 Id. 
 Id. 
 
 Id. 
 
 (Macleay), from Australia. Quart. Journ. Geol. Soc., 1859, xv., pp. 
 133 and 168-176, pls. 7 and 8. 
 
 On a Collection of Australian Fossils in the Museum of the Worcestershire 
 Natural History Society, witha Description of the Lower Jaw and 
 Teeth of Nototherium inerme (Owen), and N. Mitchelli (Owen), 
 &e. Quart. Journ. Geol, Sor., 1859, xv., pp. 176-186, pl. 9. _ 
 
 Description of some Remains of a gigantic Land Lizard, Megalania prisca (Owen), 
 from Australia [Part L] | Phil. Trans. R. Soc., 1859, exlix., pp. 43-48, 
 pls. 7 and 8. Part ei pt cit., 1881, clxxi., Pt. 3, pp. 1037-1050, 
 pls. 34-38. Part ii—Zoe. cit., 1881, clxxii., Pt. 2, pp. 547-566, pls, 
 64-66. Part iv.—Loc. cit., 1887, clxxvil., pp. 327-330, pls. 13-15. 
 
 On the Fossil Mammals of Australia, Part ii—Description of an almost entire 
 Skull of the Thylacoleo carnifex (Owen) from a Freshwater Deposit, 
 Darling Downs, Queensland. Phil. Trans., 1866, clvi., Pt. 1, pp. 
 73-82, pls. 2-4. Part ii.—On Diprotodon australis (Owen), Loc. 
 cit., elx., p. 519, pls. 35-50. Part iv.—Dentition and Mandible of 
 Thylacoleo carnifex, with Remarks on Arguments for its Herbivority. 
 
 ’ Loe. cit., 1871, clxi., pp. 213-226, pls. 11-14. Part v.—Genus 
 
 Nototherium (Owen), Loe. cit., 1872, clxii., Pt. 1, pp. 41-82, pls. 2-11. 
 Part vii—Genus Phascolomys (Geoflr.), Roe Ch 1 Sis Clete Lt 2; 
 pp, 173-196, pls. 17-23. Part vii.—Genus Diselenys eee 
 exceeding the existing ones in size. Loc. cit. 1873, clxii., Pt. 2, pp, 
 241-258, pls. 32-40. Part vili—Family Macropodide. Genera 
 Macropus, Osphranter, Phascolagus, Sthenurus, and Protemnodon. 
 Loc. cit., 1874, clxiv., Pt. 1, pp. 245-287, pls. 20-27. “Part ix.— 
 Family Macropodidw. Genera Macropus, Pachysiagon, Leptosiagon, 
 Procoptodon, and Palorchestes. Loc. cit., 1874, clxiv., Pt. 2, pp. 
 783-798, pls. 76-80. Part x.—Family Macropodide. The Mandibular 
 Dentition and parts of the Skeleton of Palorchestes, with additional 
 Evidences of Sthenurus, Macropus Titan, and Procoptodon. Loe. 
 cit., 1876, clxvi., Pt. 1, pp. 197-226, pls. 19-31. 
 
 Researches on the Fossil Remains of the Extinct Mammals of Australia, &c. 2 vols., 
 4to. London, 1877. 
 
 "On a New Species of Sthenurus [S. minor}, with Remarks on the relation to 
 
 Dorcopsis, Miller. Proc. Zool. Soc., 1877, pp. 352-361, pls. 27 and 28, 
 
 Memoirs on the Extinct Wingless Birds of New Zealand, with an Appendix on 
 those of England, Australia, &c. 2 vols., 4to. London, 1879. 
 [| Dromornis australis, Owen. | 
 
 Description of a portion of a Mandible and Teeth ofa large Extinct Kangaroo 
 (Palorchestes crassus, Owen) from ancient fluviatile drift, Queens- 
 land. Trans. Zool. Soc. 1880, xi., Pt. 1, pp. 7-10, pl. 2 
 
 On an Extinct Chelonian Reptile ( Notchelys costata, Owen) from Australia. Quart. 
 Journ. Geol. Soc., 1882, xxxviil., pp. 178-183. 
 
 Description of part of the Femur of Nototherium Mitchelli. Quart. Journ. Geol. 
 Soc., XXXvill., pp. 394-396, pl. 16. 
 
 Description of portions of a Tusk of a Proboscidian Mammal (Wotvelephas australis, 
 Owen). Phil. Trans., 1883, clxxiu., Pt. 3, pp. 777-781, pl. 51. 
 
 On the Affinities of Thyiacoleo. Phil. Trans., 1883, clxxiv., Pt. 2, pp. 575-582, 
 
 pls. 39-41. 
 Pelvic Characters of Thylacoleo carnifex. Phil. Trans., 1883, clxxiv., pp. 639-643, 
 pl. 46. 
 
 On an Outline of the Skull, basal view, of 7hylacoleo. Geol. Mag., 1883, x., p. 
 289, pl. 7. 
 
XXIV. LIST OF PAPERS. 
 
 Owen, R.—Description of Teeth of a large Extinct (Marsupial ?) Genus, Sceparnodon, Ramsay. 
 Phil. Trans., 1884, elxxv., Pt. 1, pp. 245-248, pl. 12. 
 Id. Description of Fossil Remains, including foot-bones, of Megalania prisca. Phil. 
 * Trans., 1886, clxxvii., Pt. 1, pp. 327-330, pls. 13-15. 
 Ratre, F.—Note on Crioceras Australe, Moore ? a Lower Cretaceous Fossil from Queensland. 
 Proc. Linn. Soc. N.S. Wales, 1886, i., pp. 133-135, pls. 1 and 2. 
 Srutcusoury, S.—On the Geology of the Dividing Range between the Gwydir and the Namoi, 
 Liverpool Plains District. Parl. Blue Book, N.S. Wales, Dee. 
 
 1854, pp. 14-20. 
 Id. On the Country bordering the Coast between the Rivers Brisbane and Boyne. 
 Parl. Blue Book, N.S. Wales, July, 1856, pp. 6-14. 
 Tare, R.—Description of a New Species of Belemnite from the Mesozoic Strata of Central 
 Australia. Trans R. Soc. S. Australia for 1879-80 [1880], ii., p. 
 104, pl. 4. 
 Wikinson, C. S.—Notes on a Collection of Geological Specimens from the Coasts of New 
 Guinea, Cape York, and neighbouring Islands, collected by 
 William Macleay, Esq., &c. Ann. and Mag. Nat. Hist., 1876, 
 xvill., p. 190; Geol. Mag., Dec. 2, iii., p. 428; Canadian Nat. and 
 Geol., n.8., Vill., pp. 156-160. 
 Woops, J. E. T.—On a Tertiary Formation at New Guinea. Proc. Linn. Soc. N. 8S, Wales, 
 for 1877, ii., Pt. 2, pp. 125-128. , 
 tah. On some Tertiary Fossils from New Guinea. Proc. Linn. Soc. N.S. Wales, 
 
 1878; i, Pt. 3; p.267. 
 
 Id. On a Fossiliferous Bed at the Mouth of the Endeavour River. Proc. Linn. 
 Soc. N.S. Wales, 1880, v., Pt, 2, p. 187-189. 
 
 Id. On a New Cretaceous Deposit in Queensland. 8S. Science Record, 188i, i., 
 No. 12, p. 185. 
 
 Id. On Various Deposits of Fossil Plants in Queensland. Proc. Linn. Soc. N.S. 
 Wales, 1882, vii., Pt. 1. pp. 95-98. ; ; 
 
 ie On a Coal Plant from Queensland. Proc. Linn. Soc. N.S. Wales, 1882, 
 vil., Pt. 3, pp. 342-344. 
 
 Ia. On a large Mesozoic Mytilus from the Barcoo. Proc. Linn. Soc. N.S. 
 Wales, 1882, vii., Pt. 3, pp. 389-392. 
 
 Id. On some Mesozoic Fossils from the Palmer River, Queensland. Journ. R. 
 Soc. N.S. Wales for 1882 [1883], xvi.; pp. 147-154, pls. 7, 8, and 10. 
 
 Id. A Fossil Plant Formation in Central Queensland. Journ. R. Soc. N.S. Wales 
 for 1882 [1883], xvi., pp. 179-192, pls. 11 and 12. 
 
 Id. On a species of Brachyphylium from Mesozoic Coal Beds, Ipswich, 
 
 ' Queensland. Proc. Linn. Soc. N.S. Wales, 1883, vii., Pt. 4, pp. 
 
 659-661. 
 
 Id. On the Fossil Flora of the Coal Deposits of Australia. Proc. Linn. Soc. 
 NV.S. Wales, 1883, viii., Pt. 1, pp. 37-167, pls. 1-10a. 
 
 Id. On some Mesozoic Fossils from Central “Australia. Proc. Linn. Soe. N.S. 
 
 Wales, 1883, viii., Pt. 2, pp. 235-242, pls. 12 and 13. 
 Woopwarp, A. 8.—See Etheridge, R., Junr., and Woodward, A. 8. 
 Woopwarp, H.—On the Wing of a Neuropterous Insect from the Cretaceous Limestone 
 of Flinders River, North Queensland, Australia. Geol. Mag., 1884, 
 i, pp. 337-339, pl. 11. 
 Id. Notes on some Mesozoic Plants from South Australia. Geol. Mag., 1885, ii., pp. 
 289-293, pl. 7. 
 
CONTENTS. 
 
 ——_<$-—_—_—- 
 CHAPTER I. 
 Page. 
 IntTropuctoryY sa ay are re SA 8 cat wei ney Ses - 1 
 PLUTONIC AND METAMORPHIC. 
 CHAPTER II. 
 GRANITE, SYENITE, AND Acrip CrysTALLINE Rocks. 
 Mineral Areas, viz.:—Herberton Tin Field, Kangaroo Hills and Running Creek Silver 
 and Tin Fields, Annan and Bloomfield Tin Fields, Ravenswood Gold and Silver 
 Fields, Sellheim Bismuth Mines, Croydon Gold Field, Etheridge Gold Field, 
 Kidsvold Gold Field, Mount Perry Copper Mine, Tenningering, Boolboonda, 
 Molangul, and Normanby Gold Fields, Jimna and Gooroomjam Gold Fields .., 4 
 PALAOZOIC., 
 CHAPTER III. 
 Mertamorpuic Rocks (States, Scuists, GNEISsEs, &c.), oF UNDETERMINED AGE. 
 Mineral Areas, viz. :—Cloncurry Gold and Copper Fields, McKinlay Gold Field, Charters 
 Towers and Cape Gold Fields, Gilbert and Woolgar Gold Fields, Coen Gold Field, 
 Normanby and Marengo Gold Fields, Peak Downs Gold Field, Peak Downs 
 Copper Field Jeb Tee a ne ty 55 eo a a2 ay al) 
 Devonian. 
 CHAPTER IV. 
 Mippte Devonian (Burpexin Formation). 
 Argentine Silver Field os one ae Ct, res ce as BAG sii a Oe 
 CHAPTER V. 
 Tas Orcanic Rematns or THE Mippie Devonian (Burpekin) Formation, witH 
 DEscRIPTIONS OF THE SPECIES ... Se sos os — oar aes Leys, tan 
 Permo-Carboniferous. 
 CHAPTER VI. 
 Tur Permo-CarBONIFEROUS SysTEM ... ii cde se wr ane ae Py ih 
 
 CHAPTER VII. 
 
 Tur Permo-Carponirerous SystEM—continued. Tue Gympie ForMATION IN 
 THE Typr District. 
 to fi 
 
 Mineral Areas, viz. :—Gympie Gold Field and Neerdie Antimony Mine ... “P ch YP: 
 
XXVi, CONTENTS. 
 CHAPTER VIII. 
 
 THe Prrmo-Carsonirerovs SystemM—continued. Tur Gympie Formation 
 OUTSIDE OF THE Type DrtstRIctT. 
 
 Including Yarrol, Mount Biggenden, Gebangle, Mount Shamrock, Eidsvold, Cania, Raglan, 
 Langmorn, Calliope, Kooingal, Rockhampton, Dee and Don Rivers, St. Lawrence. 
 Mineral Areas, viz.:—Kilkivan and Black Snake, Kilkivan Mercury Mines and Mount 
 Coora Copper Mine, Gayndah Gold Fields, Mount Biggenden, Gebangle, and 
 Mount Shamrock Gold Fields, Brovinia Gold Field, Paradise Gold Field, Raglan, 
 Calliope, Norton, Cania, and Kroombit Gold Fields, Rockhampton Gold Fields 
 
 (excluding Mount Morgan), Yatton Gold Field, Warwick Gold Fields 
 
 , CHAPTER IX. 
 THe Permo-Carponirerous SysteM—continued. Tue Gympie ForMATION 
 OUTSIDE OF THE Type District—continued. 
 
 Including Hodgkinson, Palmer, Mount Albion, Silverfield, Watsonville, and Chillagoe. 
 Mineral Areas, viz.:—Hodgkinson Gold Field, Northcote Antimony Mines, Mulgrave 
 Gold Field, Palmer Gold Field, Cannibal Creek Tin Field, Mitchell Antimony 
 Mines, Mount Albion and Chillagoe Silver Fields, sae River Silver Fields, Nebo 
 
 Gold Field, and Sellheim Silver Field , si Ae ; 
 
 CHAPTER X. 
 
 Tuer PreRmMo-CAaRBONIFEROUS SyYsTEM—continued. 
 The Star Formation 
 
 CHAPDERAXG: 
 Tue PrErmMo-CaRrBonirerovus SystEM—continued. 
 
 The Bowen River Coal Field and its Subdivisions 
 
 CHAPTER XII. 
 Tor PerMo-CARBONIFEROUS SysTEM— continued. 
 The Lower Bowen Formation in the Type District 
 
 CHAPTER XIII. 
 THe Permo-Carponirerovus SystemM—continued. 
 The Lower Bowen Formation outside of the Type District—Mackay District 
 
 CHAPTER XIV. 
 THe PermMo-CarBonireRous SystEM—continued. 
 The Middle Bowen Formation in the Type District 
 
 CHAPTER XV. 
 THe Permo-Carponirerous SysteM—continued. 
 The Middle Bowen Formation outside of the Type District, including Nebo, Mackay, 
 
 Banana Creek, Cracow Creek, Nogoa River, Springsure, Logan Downs, and 
 Roper Creek ... 
 
 CHAPTER XVI. 
 THE Permo-CarBoniIrerous SystemM—continued. 
 Life of the Middle Bowen Formation 
 
 CHAPTER XVII. 
 THE PrerMo-CarBonirrrous System—continued. 
 The Upper Bowen Formation in the Type District 
 
 Page. 
 
 87 
 
 113 
 
 129 
 
 143 
 
 144 
 
 146 
 
 150 
 
 159 
 
 161 
 
CONTENTS. XXVll. 
 
 CHAPTER XVIII. 
 
 THE PerMo-CarBonIFEROUS SystTEM—conlinued. 
 
 The Upper Bowen Formation outside of the Type District, including Nebo, Mackay, 
 Lenten Downs, Isaacs and Dawson’ Rivers, Cement Hill, Clermont, Blair Athole, 
 and Dinner Creek, Stanwell 
 
 CHAPTER XIX. 
 
 THE PrerMo-CaRrBONIFEROUS SystEmM—continued. 
 
 The Upper Bowen Formation outside of the Type District, continued, including Towns- 
 ville, Oaky Creek, and Little River, Cooktown ... 
 
 CHAPTER XX. 
 Tue Prermo-CarBponireRous System—continued. 
 Life of the Upper Bowen Formation 
 
 CHAPTER XXI. - 
 List oF THE FossiLs oF THE PERMO-CAaRBONIFEROUS SYSTEM, SHOWING THEIR Horizons 
 
 CHAPTER XXII. 
 
 THE OrGanic Remains or THE PerMo-CarBONIFEROUS SysTEM, WITH DeEscrIPTIONS 
 OF THE SPECIES 
 
 MESOZOIC, 
 Trias-Jura. 
 CHAPTER XXIII. 
 Tue Triss-Jura System. Lower (Burrum) Formation 
 
 CHAPTER XXIV. 
 THE Oraanic Remains or THE TrRIAS-JURA SYSTEM, WITH DESCRIPTIONS OF THE SPECIES 
 OCCURRING IN THE Burrum Formation (Lower Tartss-Jura) 
 
 CHAPTER XXV. 
 
 THE Trias-Jura System—continued. Tur Ipswich Formation (Upper Trias-JuRA) IN 
 THE Type District ... 
 
 CHAPTER XXVI. 
 
 Tue Trias-J vga SysteM—continued. Tur Ipswich Formation (Upper Trias-JurA) IN 
 THE Typre District—continued 
 
 CHAPTER XXVII. 
 
 Tue Tris-Jora SystemM—continued. Tue Ileswicn Formation (Upper Trias-Jura) Nn 
 THE Type District—continued 
 
 CHAPTER XXVIII. 
 Tue Trias-Jura SystemM—continued. Tur Ieswich Formation (UprrEr 
 Trias-J URA), OUTSIDE oF THE Type District. 
 
 Including Stewart’s Creek (Rockhampton), and Rosewood and Wycarbah (Rockhampton) 
 Beds te = it ae aa at =< fea rig Sty af 
 
 CHAPTER XXIX. 
 
 Tur Trras-Jura SystemM—continued. Tur Ipswich Formation (Upper Trras-JuURA), 
 Its Aaz AnD RELATIONS 
 
 Page. 
 
 167 
 
 189 
 
 300 
 
 333 
 
 346 
 
 . 305 
 
 359 
 
XxVill. CONTENTS. 
 
 CHAPTER XXX. 
 Tue Oreanic Remains oF THE Ipswich Formation (Upper Trias-JURA), WITH Descrip- 
 
 TIONS OF THE SPECIES ae ie ec By es sa uae es we 364 
 Cretaceous. 
 CHAPTER XXXI. 
 THE Rotting Downs Formation (Lower Creraczous)—ARTESIAN WELLS... .. 390 
 
 CHAPTER XXXII. 
 THE Orcanic REMAINS OF THE Ro~ttine Downs Formation (Lower CRETACEOUS), WITH 
 DESCRIPTIONS OF THE SPECIES ... ie ro he: ~ Ty. Se on BE 
 
 CHAPTER XXXIII. 
 Tue Desert SANDSTONE Formation (UPPER CRETACEOUS) ... soe vee Sad SeOLL 
 
 CHAPTER XXXIV. 
 THE ORGANIC REMAINS OF THE DesERT SANDSTONE Formation (Upper Cretaceous), 
 WITH DescrRIPTIONS OF THE SPECIES ee ga Rac aa a a we BODE 
 
 CAINOZOIC. 
 Tertiary. 
 CHAPTER XXXV. 
 Lower (Miocenr?’) anp Uprrr (Pirocenre?) Votcanitc Rocks anp Drirts. 
 Russell River and Mulgrave Gold Fields, Mount Morgan Gold Mine, Moondilla Gold Field 575 
 
 Post-Tertiary. 
 CHAPTER XXXVI. 
 
 Post-Trrtrary AnD Recent. Caves. Ratsep Beacnes. Sanp Dunes. ‘THERMAL 
 AND OTHER SPRINGS. 
 
 Stanniferous Drifts, viz. :—Stanthorpe, Mount Spurgeon, and Pascoe Tin Fields we §©604 
 CHAPTER XX XVII 
 
 Tue Organic REMAtNS OF THE Post-TertTIARY PERIOD me ann ae nie So at 
 CHAPTER XXXVIITI. 
 
 Gerotogy or British New Guinea ae Bc ec Ree ae Ei nee se. 004 
 
 CHAPTER XXXIX. 
 
 PaLtzontoLocy oF New GUINEA ... Nee .. 690 
 
 CHAPTER XL. 
 PerrograpHicat Notes ON SPECIMENS FROM QUEENSLAND AND ADJACENT COLONIES, BY 
 Ae W. CrARKE, F.G.S. eee eee eee eee eee ene eee eee eee 699 
 
bo 
 
 “gf 9 
 
 >) | 
 
 CO OO” EST ror 
 
 LIST OF PLATES. 
 
 —_—_ >—__—_—— 
 
 . Devonian Corals. 
 
 . Devonian Corals. 
 
 . Devonian Corals. 
 
 . Devonian Mollusea and Devonian and Permo-Carboniferous Plants. 
 . Permo-Carboniferous Plants. 
 
 . Permo-Carboniferous Plants and Corals. 
 
 : Permo-Carboniferous Corals, Echinodermata, and Crustacea. 
 
 . Permo-Carboniferous Annelida, Echinodermata, and Polyzoa. 
 
 . Permo-Carboniferous Polyzoa and Brachiopoda. 
 
 10. 
 a1: 
 12. 
 138. 
 14. 
 15. 
 16. 
 1%. 
 18. 
 19. 
 20. 
 21, 
 22. 
 23. 
 24. 
 25. 
 26. 
 27. 
 28. 
 29. 
 30. 
 
 Permo-Carboniferous Brachiopoda. 
 Permo-Carboniferous Brachiopoda. 
 Permo-Carboniferous Brachiopoda. 
 Permo-Carboniferous Brachiopoda. 
 Permo-Carboniferous Brachiopoda, Pelecypoda, Gasteropoda, and Cephalopoda. 
 Permo-Carboniferous Gasteropoda and Cephalopoda. 
 Permo-Carboniferous and Mesozoic Plants. 
 Permo-Carboniferous and Mesozoic Plants. 
 Permo-Carboniferous and Mesozoic Plants. 
 Cretaceous Spongida. 
 
 Cretaceous Echinodermata, Insecta, and Mollusca. 
 Cretaceous Pelecypoda. 
 
 Cretaceous Pelecypoda. 
 
 Cretaceous Pelecypoda. 
 
 Cretaceous Pelecypoda. 
 
 Cretaceous Pelecypoda. 
 
 Cretaceous Pelecypoda. 
 
 Cretaceous Pelecypoda. 
 
 Cretaceous Pelecypoda. 
 
 Cretaceous Gasteropoda and Cephalopoda. 
 
 Cretaceous Cephalopoda. 
 
XxX. 
 
 31. 
 
 LIST OF PLATES. 
 
 Cretaceous Gasteropoda and Cephalopoda. 
 
 . Cretaceous Cephalopoda. 
 33. 
 34, 
 35. 
 36. 
 37. 
 38. 
 39. 
 40. 
 Al. 
 
 Cretaceous Pelecypoda and Cephalopoda. 
 
 Cretaceous Pelecypoda and Cephalopoda. 
 
 Cretaceous Cephalopoda. 
 
 Tertiary Corals and Post-Tertiary Mollusca and Crustacea. 
 Devonian and Permo-Carboniferous Corals and Mollusca. 
 Permo-Carboniferous Corals, Brachiopoda, &e. 
 Permo-Carboniferous Brachiopoda, Cephalopoda, &c. 
 Permo-Carboniferous Mollusca. 
 
 Permo-Carboniferous Mollusca. 
 
 . Cretaceous Mollusea and Mesozoic Plants. 
 atey 
 44, 
 
 Permo-Carboniferous and Cretaceous Mollusca. 
 
 Permo-Carboniferous Miscellanea. 
 
 . Geological Sections. 
 . Geological Sections. 
 . Geological Map of the Burrum Coal Field. 
 . Geological Map of the Gympie Gold Field. 
 . Geological Sections. 
 . Geological Sections. 
 . Geological Sections. 
 . Geological Sections. 
 
 . Geological-Sections. 
 
 54 & 55. Sections across Gympie Gold Field. 
 
 56. 
 57. 
 58. 
 59. 
 
 Section across Gympie Gold Field. 
 
 Section across Gympie Gold Field. 
 
 Section across the Two-Mile, Gympie Gold Field. 
 Plan of Charters Towers Gold Field. 
 
 60-68. Petrographical Sectiors. 
 
 69. 
 
 Geological Map of Queensland, in six sheets. 
 
ERRATA. 
 
 N.B.—The pagination is counted as a line. 
 
 PAGE. 
 7.—Line 33, for “ Creek” read “ River.” 
 
 10.—Line 35, for “ CrerKk”’ read “ River.” 
 sy 
 
 21.—After extract from Brisbane Courier referring to Last Call Mine, Cloncurry, refer to Note at foot 
 of p. 149. 
 
 72.—Line 24, for “‘bisucleata” read “ bisuleata.” 
 73.—Second footnote, for ‘‘ Durandin” read “ Duranduyr.”’ 
 112.—Last line, dele ‘ Aplin.” 
 159.—Line 34, for “ duodecemcostata ” read ‘‘ duodecimeostata.”’ 
 170.—Line 9, for “ Lower” read “ Middle.” 
 193.—Last line, for “ No. 5”’ read “ No. 8.” 
 245.—Transfer first footnote to bottom of page 244. 
 269.—Line 23, for “ ILLAWARENSIS ” read “‘ ILLAWARRENSIS.” Line 26, for “p. 301” read “p. 163.” 
 273.—Line 42, for “‘ R. L. Jack” read “ The late James Smith.” 
 274.—First footnote, before Macrodon insert =. 
 308.—Line 25, for “A” read “ W.” 
 311.—After line 44 add as in Appendix VIII. 
 312.—Line 39, for “twelve” read “ thirteen,” and for “ four” read “ five.” 
 315.— After line 23 add as in Appendix IX. 
 394.—Line 23, for “ B. Canhami”’ read “‘ Belemnites Canhami.” 
 397.—Line 4, for “ Selheimi” read “ Sellheimi.” Line 14, for “ apendiculatus” read “ appendieulatus.” 
 401.—Line 27, dele “ Cloncurry.” 
 406.—Lines 6 and 8, for “ Crispii” read “ Cripsii.” 
 428.—At end of first footnote insert “ R.Z.J.”’ At end of second footnote insert ‘ J. B.H.” 
 434,—Line 5, for “ Bed” read “ Beds.” 
 457.—Line 3, for “ Pl. 20, figs. 1, 3, 5, 7, and 10” read “ Pl. 23, figs. 3, 5,7, and 10, ? figs. 1 and 2.” 
 475.—Line 29, for “ Macrocallista Taylori” read ‘‘ Macrocallista plana.” 
 478.—Line 12, for “‘ PAL HOMZARA” read “PALHOM@RA.” Line 14, for “ PatnommRa”’ read 
 “ PALEZOM@RA.” 
 490.—Line 3, for “‘? Plate 39’ read “? Plate 29.” 
 511.—Line 40, for ‘‘ Down” read “ Downs.” 
 512.— Line 31, for “ Mitchell” read “ Maranoa.” Line 82, for “ following” read “ foregoing.” 
 549,—Line 8, for “ parallel’’ read “ meridian.” 
 644.—Between lines 35 and 36 add “ Limyma vinosa, A. Adams and Angas.” 
 672.—Line 38, for “ Strutchbury ’’ read “ Stutchbury.” 
 736.—Third line of footnote, after “crystals” insert “ of augite.” 
 
= 
 
 
 
GEOLOGY AND PALAONTOLOGY OF QUEENSLAND 
 AND NEW GUINEA. | 
 
 —_@—_——_- 
 
 CHAPTER LI. 
 INTRODUCTORY. 
 
 THE eastern third, or perhaps nearly the half, of Queensland is the remnant of a 
 lofty tableland, composed of hard materials which have resisted denudation, and which 
 culminates, at an elevation of 5,150 feet, in the Bellenden-Ker Ranges.* This table- 
 land is the chief seat of the mineral wealth of the Colony. Its eastern edge presents 
 a series of escarpments, or a short and steep slope down to the Pacific. This elevated 
 tract generally robs the rain-charged clouds which rise up-from the ocean, and a fairly 
 watered and well-timbered country is the result. The generally indifferent character of 
 the soil accounts for the fact that the grasses, although fair, are not first-rate for 
 pastoral purposes. Where, however, basaltic plateaux occur, agricultural soils of the 
 highest quality are produced, and are often covered by dense tropical jungles, watered 
 by copious and perennial streams. 
 
 Besides granites and syenites, partly of plutonic and partly of metamorphic 
 origin, and basic igneous rocks, both bedded and intrusive,and of various ages, this coast 
 region contains a series of stratified rocks, of which the older members are more or less 
 metamorphosed. Among these, and recognisable by their fossil contents, are formations 
 related homotaxially to the Middle Devonian (Burdekin), the Permo-Carboniferous 
 (Gympie, Star, and Lower, Middle, and Upper Bowen), the Trias-Jura (Burrum and 
 Ipswich), the Cretaceous (Rolling Downs and Desert Sandstone), the Miocene and 
 Pliocene (Lower and Upper Volcanic Series with associated Drifts), the Post-Tertiary, 
 and the Recent. 
 
 The western interior presents a totally different aspect. The tableland slopes 
 gradually westward and falls away towards the Gulf of Carpentaria and the south- 
 western boundaries of the Colony. The greater part of the interior is covered by soft 
 stratified rocks of Cretaceous age which weather into a fine soil, supporting nutritious 
 grasses, but almost treeless except in the south-western districts, where thick scrubs of 
 mulga and gidya cover a region which is perhaps partly of Tertiary age. The rainfall 
 over this area is, however, comparatively small, and the watercourses are ill-defined and 
 dried up to waterholes during the greater part of the year. This defect on the part of 
 nature is rapidly being remedied by the sinking of artesian wells. At intervals portions 
 of the interior are occupied by detached tablelands of what has been aptly named 
 “ Desert Sandstone,” supporting, as a rule, only spinifex grass and stunted timber. The 
 
 
 
 * Report on the Bellenden-Ker Range, North Queensland, by A. Meston. Fep. Brisbane: by 
 Authority : 1889, 
 
2 
 
 evidences that the Desert Sandstone once covered the whole of the western interior are 
 unmistakable, and it is matter for congratulation that it has been so extensively 
 denuded as to lay bare, over an immense area, the rich soil-producing Cretaceous rocks. 
 Between the Desert Sandstone and the Recent deposits is a series of drifts containing 
 the remains of extinct marsupials and other animals. 
 
 In the following chapters, the various formations which tell a part of the 
 geological history of the Colony are described in detail. 
 
 In my “ Handbook of Queensland Geology” (Brisbane, 1886), of which the 
 present work may to some extent be regarded as an expansion, I favoured the use of 
 local names for the various formations described. In the present work, although the 
 local names have been for the most part retained, I have ventured to point out the 
 probable relations of the Queensland formations to those of Europe. 
 
 In a highly philosophical essay, Mr. R. M. Johnston, F.L.S., Government 
 Statistician of Tasmania, asked the members of the Australasian Association* the 
 question, ‘‘ How far can Australian geologists safely rely upon the order of succession 
 of the characteristic genera of fossil plants of a far distant region in the determination 
 of the order and relationship of Australian terrestrial formations ?’’ and answered for 
 them, that—‘‘Australian geologists cannot with safety so rely, and that even within the 
 wide borders of Australia considerable differences may be expected in the biology and 
 minor subdivisions of systems as developed in some of its widely separated colonies.” I, 
 for one, heartily concur in this verdict, and I know that my Colleague in the paleontological 
 work has been fully alive to the difficulties attending classification wben based upon 
 paleobotanical evidence alone. In dealing with animal remains, however, we trace a 
 parallelism between the formations of Australia and Europe, although in view of the 
 wide distance between the two regions we do not claim more than homotaxial relationship 
 for the formations to which in Queensland we have attached European names. We 
 must, however, point out that the order of succession of the Queensland formations 
 bears a general and striking resemblance to that of the European. 
 
 These sedimentary formations are described in the order indicated in the following 
 table, commencing with the oldest or lowest. 
 
 
 
 * Proc, Austr. Assoc, Ady: Sci. for 1888 [1889} p. 302, 
 
3 
 
 CLASSIFICATION AND SUPPOSED AFFINITIES OF QUEENSLAND FoRrMATIONS. 
 
 
 
 FORMATIONS. 
 
 
 
 Recent and Post-Pliocene 
 
 Recent Alluvia 
 
 Sand Dunes 
 
 Raised Beaches 
 
 High-level River and Lake Drifts 
 Cave Breccias 
 
 Bone Drifts 
 
 Post-TERTIARY 
 a . 
 Post-Pliocene 
 
 | Upper Volcanic, and Drifts (? Pliocene) 
 
 TERTIARY. 
 
 OI I sar ane Y 
 Pliocene 
 
 
 
 o 
 eA 
 = \ Lower Volcanic, and Drifts (? Miocene) 
 - 
 22222 ODDO DDOODDODODO DOOD DOD RADA OOD ODS OM! 
 = » 
 Ria Desert Sandstone 
 =| 
 Ps 
 === PPO P GE 59 0950 5654-446444446444644444- 
 <a 
 ++ 
 . o 2 5 
 ~ ES Rolling Downs 
 N aa 
 o 
 a 3 
 si ais Ipswich 
 3 
 PS PPAAIHAD IDEA AE IL EDIE ETH ET EOE 
 B.S 
 am Burrum 
 “= 
 
 Upper Bowen 
 
 
 
 Middle Bowen 
 
 
 
 Lower Bowen 
 
 DO HHH HHI 
 Star 
 
 DDD D4DG4444-4-4-4 4-44-44 4444444644446464646 
 
 Permo-Carboniferous 
 
 Gympie 
 
 PaLzozoic. 
 
 Burdekin 
 
 Middle i ; 
 Devonian. 
 
 
 
 Slates, Schists, &c., of undetermined 
 age 
 
 
 
 Silurian ? 
 Cambrian ? 
 Laurentian ? 
 
 lam 
 
 
 
 Nore, #¢¢¢+#4 denotes an unconformable succession 
 
 
 
CHAPTER II. 
 
 PLUTONIC AND METAMORPHIC ROCKS. 
 
 (GRANITE, SYENITE, AND ACID CRYSTALLINE ROCKS.) 
 
 Mineral Areas—viz., Herberton Tin Field, Kangaroo Hills and Running Creek Siiver and Tin 
 Fields, Annan and Bloomfield Tin Fields, Ravenswood Gold and Silver Fields, Sellheim 
 Bismuth Mines, Croydon Gold Field, Etheridge Gold Field, Eidsvold Gold Field, Mount 
 Perry Copper Mine, Tenningering, Boolhoonda, Molangul, and Normanby Gold Fields, 
 Jimna and Gooroomjam Gold Fields. 
 
 In denoting the whole of these rocks, on the ground of their lithological relationship, by 
 a single colour, I am well aware that the highest purpose of a geological map is not 
 served, but it seems all that can be done until a great amount of detailed surveying, 
 accompanied by micro-petrographical study, can be carried out. 
 
 In some regions the Granites and Syenites are clearly metamorphic. In others, 
 whether originally of metamorphic or of plutonic origin, they are covered by the 
 oldest fossiliferous deposits of the Colony. Sometimes they are intruded among 
 the earlier rocks. Sheets of quartz-porphyry in the neighbourhood of Townsville 
 have been intruded among rocks containing Glossopteris, and presumably of the age 
 of the Bowen River Coal Field. The Hon. A. C. Gregory refers* to “the extensive 
 development of the porphyritic rocks which, rising through the Carbonaceous strata 
 [Ipswich J*ormation], form the range dividing the valley of the Mary River from the 
 Maroochy River.” 
 
 The same Author thus refers to the porphyries of the Moreton and Darling 
 Downs districts +:—“ The porphyry consists of a pale-brown paste with minute 
 felspathic crystals, though it sometimes varies so as to consist of very small grains of 
 quartz with minute cavities, containing oxide of iron, resulting from the decomposition 
 of pyrites. Occasionally it is vesicular, and has the aspect of trachyte. 
 
 “The age of this rock is greater than that of the basalts, which cut through and 
 overlay it, though it often occurs that the basalt has found vent through the same 
 fissures as the porphyry, and formed spurs to the more elevated masses of the older 
 igneous rock, a feature which is especially developed on both sides of the Main Range, 
 near Cunningham’s Gap, where Mount Cordeaux, Mount Mitchell, and Spicer’s Peak 
 are porphyry, and the subordinate ranges basaltic. 
 
 “On the other hand the age is less than that of the Carbonaceous Series [Ipswich 
 Formation], as the porphyry in all cases is found superimposed on the sedimentary 
 strata. 
 
 *‘The porphyritic rock is chiefly developed in the southern portion of the 
 Moreton district, where it forms all the remarkable peaks on the Great Dividing Range 
 from the head of Laidley Creek to the southern boundary of the Colony, and thence 
 along the Macpherson Range, which separates the Logan River from the Clarence, 
 Richmond, and Tweed Rivers. 
 
 
 
 * Report on the Geology of part of the District of Wide Bay and Burnett. TF cp. Brisbane: by 
 Authority : 1875. 
 
 + Report on the Geological Features of the South-eastern Districts of Queensland. Fcp. Brisbane ; 
 by Authority : 1879. 
 
5 
 
 “ The general aspect of these hills is a suecession of sharp peaks, formed by the 
 upheaval of portions of strata, with a change of angle, one side of each hill being a 
 nearly even slope, with a steep escarpment on the opposite side. The steep side, 
 however, shows a columnar structure, which is vertical, and not a right angle, with the 
 slope on the opposite side of the hills. Some of these peaks, as Mount Barney, 
 Wilson’s Peak, Mount Lindsay, and Mount Mitchell, have an altitude of 3,000 and 4,000 
 feet, and show the porphyry to exceed 2,000 feet, but in every case resting on car- 
 bonaceous rocks [Ipswich Formation]. Though the porphyry sometimes flowed over 
 considerable areas in thin sheets, and shows a cellular structure, yet the greater part 
 must have been less fluid when erupted than the basalts. 
 
 “ Besides the principal mass between Cunningham’s Gap and Mount Lindsay, 
 there are several detached points of eruption, as Knapp’s Peak, Mount French, Mount 
 Edwards, Flinders Peak, and Mount Goolman, all situate to the south of Ipswich, 
 Mount Esk, on the Upper Brisbane River, Kangaroo Point, Bowen Terrace, and 
 Spring Hill, in the town of Brisbane; also the Glasshouse Mountains. 
 
 “Tn the town of Brisbane the porphyry is erupted through the Devonian slate, 
 fragments of which are disseminated through the porphyry, while portions of silicified 
 wood are embedded in the lower surface of the erupted mass.” 
 
 In another place it will be seen that the Kangaroo Point and Bowen Terrace rock 
 is regarded as an altered brecciform ash rather than as a true crystalline rock. The 
 Glasshouse Mountains, also, were regarded by Stutchbury as altered sandstone. 
 
 The granite of the Pentland Hills is metamorphic, “alternate layers of coarser 
 and finer material betraying its originally sedimentary origin,”’ as has been observed by 
 Daintree, and subsequently by myself. 
 
 As many of the most important metalliferous fields of the Colony occur in the 
 group of rocks now referred to, lithological observations will be found in the descriptions 
 of the localities. The reader is also referred to Mr. A. W. Clarke’s Micro-Petrographical 
 Notes printed with this work. 
 
 MINES CONNECTED WITH GRANITIC, &c., ROCKS. 
 HERBERTON TIN FIELD. 
 
 This field, which is one of the most important sources of lode tin in Australia, was 
 only discovered in 1879. ; 
 
 The “ country-rock” of this field is divisible into three classes: (1) a perfectly 
 normal granite; (2) a porphyry of quartz and felspar (quartz predominating), with 
 mica as an occasional or accidental and not essential constituent; and (3) highly inclined 
 greywackes, quartzites, and shales—belonging, there is every reason to believe, to the 
 Gympie Formation. The rocks of the first class, which extend northward from Watson- 
 ville, appear to be nearly barren of tin ore, at least in the neighbourhood of Herberton 
 and Watsonville, although at Return Creek they contain tin lodes. Those of the second 
 were for a time regarded as the only seat of the tin deposits; but it is now questionable 
 whether those of the third class do not excel them in this respect. 
 
 The porphyry rocks are intersected in every direction by large “elvan” dykes 
 (compact, highly silicated, yellowish or greenish felspar base, with blebs of quartz).* 
 These elvans contain a good deal of arsenical pyrites, but—except in the case of the 
 Three Star Mine—have not yet proved to be tin-bearing to any great extent. Dykes of 
 quartzose chlorite and quartzose serpentine—probably originally intruded among the 
 porphyry as quartz-diorites, or as rocks more or less of basaltic type, and subsequently 
 
 
 
 * See Mr. Clarke’s Micro-Petrographical Notes, 
 
6 
 
 . 
 
 nietamorphosed—form the chief matrix of the tin ore in the porphyry country. The 
 ore (binoxide of tin) occurs in floors, veins, or pipes, among the joint-planes of the 
 dykes. It is rarely crystalline; but occurs either in amorphous masses, almost 
 chemically pure, or intermixed with the dyke rock. Sometimes, as in the Bradlaugh 
 Mine, the ore is so finely disseminated through the dark chlorite matrix as not to be. 
 distinguishable by the naked eye. These “chlorite ores’’ generally weather of the 
 colour characteristic of iron peroxide, and in such cases the tin ore is rather more 
 obvious. Fluorspar and wolfram are associated with the ore, but tourmaline is of rather 
 rare occurrence. 
 
 It seems most probable that the tin first came up in solution after the consolida- 
 tion of the dykes and has been deposited along their walls and among the fissures and 
 joint-planes which traversed them. A re-solution of the tin ore probably took place 
 simultaneously with the metamorphism of the dykes; and as the metamorphosed dykes 
 had probably a new joint system developed in them, a further concentration of the ore 
 may have taken place. 
 
 Considerable difficulties were at first experienced in following down the apparently 
 capricious ore deposits, and the miners were haunted by doubts as to their continuance 
 at greater depths. It has always seemed to me that their intimate connection with 
 dykes was a sufficient guarantee of their great vertical range. The Great Northern, 
 which has maintained from the beginning its position as the leading mine in the porphyry 
 country, is now turning out ore from the 400-feet level. 
 
 In the sedimentary country-rock the group of mines now united in the North 
 Australian Lease, near Watsonville, was the first to attract attention. In these mines, 
 especially in the North Australian and Ironclad, the lodes, although themselves some- 
 times poor for a distance, sent off huge “carbonas” of tin and copper ore along the 
 bedding-planes of the shales and greywackes. In 1883-6, this group of mines yielded 
 1,287 tons of dressed tin ore, valued at £64,382. Important discoveries of silver and 
 copper ores in this country have recently been reported. 
 
 More recently very important lodes of tin ore have been opened up in the 
 sedimentary rocks at Irvinebank (Great Southern, &c.), in Glen Linedale, and at 
 Denny and Dogherty’s Camp. In the Irvinebank lodes the ore is generally of the 
 “chlorite” type, and in the Great Southern Mine it is associated with arsenical pyrites, 
 bismuth, stibnite, &c. In the Gordon, in Glen Linedale, the ore impregnates a country- 
 rock of hard, fine-grained, siliceous, and talcose sandstone. At Denny and Dogherty’s 
 Camp very fine crystals of tin ore are disseminated through a chloritic matrix in lodes 
 which coincide with the bedding of the country-rock (pebbly grits). 
 
 There is little doubt that the stanniferous sedimentary rocks of this district are 
 part of the same mineralised belt which has produced the lead and silver ores of Mount 
 Albion and the Dry River. 
 
 Considering the amount of lode tin obtained in the district, the yield of stream 
 tin has been insignificant. A. considerable quantity, however, has been taken from a 
 deep lead covered by basalt in the valleys of Nigger Creek and the Wild River. 
 
 For detailed information regarding the lodes the reader may be referred to— 
 
 (1) Report (R.L.J.) on the Wild River Tin Mines, 27th October, 1880, in 
 Further Reports on the Progress of the Gold Prospecting Expedition in 
 Cape York Peninsula, 1881. 
 
 (2) Report (R.L.J.) on the Tin Mines of Herberton, &c., 1883. 
 
 (3) Report (R.L.J.) on Mineral Lease 276 (North Australian), Watsonville, 
 1887. 
 
 (4) Report (R.L.J.) on the Chillagoe and Koorboora Mining Districts, 1891. 
 
7 
 
 (5) Report (A. Gibb Maitland) on the Coolgarra Tin Mines and Surrounding 
 District, 1891. 
 
 (6) Mineral Lands Commissioner’s Reports in Annual Reports of the Depart- 
 ment of Mines. * 
 
 YIELD or HERBERTON TIN FIELD. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 LODE TIN ORE. 
 Str - 5 
 Year. ae nae ih oe Total. Value. Remarks. 
 Crushed. Black Tin. 
 
 : Tons. Tons. Tons. Tons cwt. £ 
 
 *1879 a wee ahes 131 9 5,260 | Exported 
 
 *1880 sa ee ee 193 11 7,740 . 
 
 *1881 ane ace asia 1,183 10 4/7340 3 
 
 *1882 si ae 1,810 2 72,400 3 
 
 +1883 12,405 2,646 sae ae Raised 
 
 +1883 Bogging 100 oe 3,346 0 109,740 ¥ 
 
 +1883 ae nes 600 25,200 7 
 
 +1884 11,031 1,902 road: 68,474 
 
 +1884. & * 450 § 2,302 071 16900 | |, 
 
 +1885 12,834 2,096 250 2,346 O 117,787 | Raised; 651 tons black tin 
 smelted at Irvinebank yielded 
 438 tons tin 
 
 +1886 14,811 2,198 a 2448 0 109,920 | Raised; 666 tons black tin 
 
 +1886 7 ay 250 i 13,000 smelted at Irvinebank yielded 
 416% tons tin 
 
 +1887 12,142 1,508 300 1,808 0 126,560 | Raised 
 
 +1888 11,159 1,390 Tura 1,561 0O 78,150 . 
 
 +1889 14,476 1,561 * 258 3 kod) 90,900 ae 
 
 +1890 13,700 1,690 341 2,031 O 104,050 x 
 
 Totals| ... 21,028 12 992,721 
 
 
 
 
 
 
 
 
 
 KANGAROO HILLS AND RUNNING CREEK TIN AND SILVER FIELDS. 
 
 Stream tin ore has been worked on Running Creek as far back as 1875, but no 
 records of the output are now obtainable. The following account of this district is 
 taken from a Report ft on the Geology and Mineral Resources of the Upper Burdekin, by 
 Mr. A. Gibb Maitland :— 
 
 “There is no map in existence showing the relations which the various claims 
 and creeks on the Kangaroo Hills Tin Field bear to one another. 
 
 “The larger portion of the stream tin workings exists near the confluence of 
 Sandy and Prospectors’ Creeks—tributaries of Oakey Creek—at an estimated altitude, 
 by aneroid, of 2,113 feet above the level of the sea. 
 
 “ At the time of my visit to the field, in June, 1890, it was practically deserted. 
 A few men were at work. In some cases the creeks and gullies were being ‘raked’ for 
 the second or third time. 
 
 “The ore of tin obtained throughout the field is the binoxide (cassiterite), which 
 occurs in rounded fragments and broken crystals, generally of a reddish colour, and of 
 
 no very great size. In some of the claims I saw a few of an amber colour, but they 
 did not appear to be very common. 
 
 
 
 
 
 * From Return to the Legislative Assembly of Tin Ore exported from Tinaroo District, 1886, 
 + From Mineral Lands Commissioner’s Report in Annual Reports of the Department of Mines, 
 t Fep. Brisbane: by Authority: 1891. 
 
8 
 
 ‘¢ Along with the tin in the wash there were a few topazes and a little magnetite. 
 
 “The washdirt rests directly upon an uneven surface of granite. A section of 
 this is well seen in a claim, originally part of the old P.C., viz. :— 
 
 (a) Stratified gritty sand, of a yellowish red colour, with a somewhat gravelly 
 base, and varying in thickness from 10 to 14 feet. 
 (6) Cement, the matrix being a clay of a bluish-white colour, though often 
 stained yellow. Of this there are from 8 to 4 feet. 
 It is in this cement, which contains boulders of rocks of the same nature as that forming 
 the surrounding country, that the cassiterite occurs in irregular patches. A small 
 quantity of tin, but of no commercial importance, is met with in the upper stratified 
 sand. It is a noteworthy circumstance that the ground to the south of Prospectors’ 
 Creek contains a fair quantity of tin in the surface débris, but, as yet, search has failed 
 to discover the lode from which the tin erystals undoubtedly came. 
 
 “There are reefs and dykes from which tin has been derived, scattered over a 
 fairly wide extent of country; but upon none of them has any great amount of work * 
 been done up to the present. Some of the dykes bear a marked resemblance to those in 
 the Western and Coolgarra districts. 
 
 “These dykes are intrusive basic igneous rocks. So far as is at present known, 
 these do not attain any very great thickness, nor does their horizontal extension appear 
 in this district to be very great. 
 
 “Two leases have been taken up—the 40-acre lease, and the 60-acre lease; these 
 are situated about 8 to 9 miles east from Kangaroo Hills Station. 
 
 “Tn the 40-acre lease, situated on the eastern bank of the gully, a tributary of 
 the Douglas, a cutting has been put in on the face of the hill upon a tin-bearing lode in 
 granite country, which appears to trend north-east and south-west. A section across 
 this lode shows on the north about 30 inches of gangue made up of quartz and chlorite, 
 with the binoxide of tin disseminated through it. Small quantities of the blue and 
 green carbonates of copper are also contained in the gangue. Adjoining this to the south 
 there is a thickness of about 30 inches of quartz. A thin film of serpentine separates 
 the quartz from the gangue. 
 
 “A few yards up the hill another cutting has been put in with the object of 
 following a vein running N. 65° E. The matrix of the vein is similar to that above 
 described. 
 
 “ Near the head of the gully an open work shows a wedge-shaped mass of quartz 
 and chlorite trending due east. Both walls are granite, the faces of which are often 
 coated with the green carbonate of copper. Some very large crystals of cassiterite 
 could be seen in the quartz lying near the surface. 
 
 “ Still further up the creek a shallow shaft has been sunk upon a vein which has 
 a course of N. 30° E. The vein hasa thickness of from 1 to 12 inches. Hematite, 
 limonite, and iron pyrites occur associated with the quartz and tin. 
 
 “The 60-acre lease lies some distance west of the last. Upon it a shaft has 
 been sunk to a depth unknown to my informant. 
 
 “Tn the shaft a leader with a general course of north-east and south-west is 
 met with. 
 
 “Where the shaft now stands a good bunch of tin-bearing gangue, about 2 feet 
 G inches across, has been met with. The gangue is quartzose chlorite of a nature 
 similar to that met with throughout the district. 
 
 ‘West of the shaft an open work shows a good leader of variable thickness 
 underlying to the north and trending east and west. The open work, 20 feet in depth 
 and now full of water, is reputed to have yielded a fair quantity of tin ore. 
 
9 
 
 “The only returns of the output of the tin ore from this field are scattered 
 through the annual reports of the Mines Department and the records kept in the 
 Custom House, Dungeness. 
 
 “The following is a Tabulated Statement of the Yield of Tin from the 
 Kangaroo Hills District, so far as can be obtained. This table includes the yield from 
 the recently discovered alluvial field in Dingo Creek, distant about 30 miles from . 
 Kangaroo Hills :— 
 
 
 
 
 
 
 
 Year. Yield of Black Tin, Value, Authority. 
 Tons cwt. 25 
 1885 100. O 5,556 | Mineral Wealth of Queensland. 
 1886 ial @ 6,534 | Annual Report, Mines Department, 1886. 
 1887 83 «6 300 Customs Records, Dungeness. 
 1888 117 16 ” PP ” 
 1889 137% 0 5 Fe . 
 1890 38 60 . - 
 
 
 
 
 
 ** Bismuth.—Fragments of carbonate of bismuth have been discovered in the 
 alluvial gravels in the neighbourhood of Kangaroo Hills. Recently bismuth has been 
 met with in one of the creeks draining into Halifax Bay. 
 
 “ Tron.—Ores of iron are very plentiful throughout the district. 
 
 “In one of the branches of Biscuit Creek, about 9 miles down the river below 
 Kangaroo Hills Station, there is a large lode of hematite in quartz country. The ore 
 has a considerable disturbing effect on the magnetic needle. 
 
 ‘Some distance north of Donnybrook there occurs what is known as the Iron 
 Mountain. ‘This rises to an altitude by aneroid of 200 feet above the level of the camp 
 at Donnybrook. 
 
 “The Iron Mountain in reality occupies one end of the cap of a lode which can 
 be traced for some distance. 
 
 “Tn places there is a kind of quartzose gangue. At one spot huge blocks of- 
 hematite and limonite stand out in bold relief upon the back of the lode. 
 
 “The general course of this lode is north-west and south-east. Numerous 
 veinlets branch off at right angles to the strike. At one place merely small bunches 
 and veinlets of hematite occur in the gangue, in addition to small quantities of the 
 blue and green carbonates of copper. 
 
 “Near the ‘ Mountain’ the lode or mass presents a steep escarpment to the 
 east. 
 
 “On the face green and blue carbonates of copper form botryvidal and stalactitic 
 masses in a cavern about 9 feet in height, which runs for a few feet westwards. 
 
 ** Along the whole course of ae lode a little surface-work has been done, and 
 this seemed to show that the general character of the ore is the same throughout its 
 whole length. The linear persistence of this lode is most marked.” 
 
 *¢ SinvERr-LEaD. 
 
 “A promising deposit oceurs about 25 miles distant southwards from 
 Kangaroo Hill Station at a place known as Donnybrook, on the waters of the 
 Running River. 
 
 “The discovery is said to have been made by Mr. R. Moss, one of the present 
 owners, when out on a prospecting trip in the year 1871, but until the year 1890 he 
 »took no steps to work the deposit. 
 
 ® 
 
10 
 
 ‘At the time I visited Donnybrook, in June of 1890, Mr. Moss was the only one 
 in the field. Little or no work could be said to have been done ; hence to examine the 
 surface features was all that could be done. The deposit occurs amongst a series of 
 quartzites and saccharine limestones, the age of which, in the absence of detailed 
 mapping or fossil evidence, I would hesitate to fix. From such an examination as was 
 made, the limestones did not appear to occupy any very great extent of country, and 
 the whole of the rocks appeared to have undergone a certain amount of faulting and 
 disturbance, resulting in the production of fissures of variable dimensions in which the 
 ores were deposited. 
 
 “ About half-a-mile north of the camp at Donnybrook a shaft has been put down 
 to no great depth upon a lode of galena of variable thickness. The hanging-wall is 
 well-defined, while the foot-wall cannot be said to have yet been found. A greyish- 
 blue limestone forms the hanging-wall. The course of the lode appears to be about 
 N. 20° E. In the cap were a little green and blue carbonate of copper and cerussite, 
 with kernels of galena. The lead is said to assay about 53 oz. of silver to the ton. 
 
 “A little to the north a similar galena lode had been opened up; this is said to 
 assay 26 oz. of silver to the ton. Very little work had been done at the time of my 
 visit. The ore at the surface contains green and blue carbonates of copper, galena, and 
 carbonate of lead. One of the walls is a white saccharine limestone which runs 
 N. 65° E. . 
 
 “ Close to Donnybrook, the most work appears to have been done upon a lode 
 known as the Hidden Treasure. A shaft has been put down to a depth of 40 feet. No 
 foot-wall appeared to have yet been met with. 
 
 “The lode consisted of a large body of kaolin and lithomarge, containing 
 small quantities of green carbonate of copper, some showing native silver fairly 
 abundantly, and a little oxide of manganese (hausmannite ?). A specimen from 
 the surface, containing cerussite and copper carbonates, assayed for me by Messrs. 
 Coane and Clarke, yielded 314 oz. 5 dwt.1 gr. of silver to the ton and 19 per cent. 
 of lead. 
 
 “ At the foot of the shaft galena was beginning to make its appearance at 45° 
 to S. 60° E. The galena, of fairly fine grain, yielded, on assay by Messrs. Coane and 
 Clarke, 1 oz. 9 dwt. 9 gr. of silver to the ton and 28 per cent. of lead, with a trace of 
 
 old.”’ 
 : Since Mr. Maitland’s report was written it appears that the Running Creek 
 Silver Mines are about to become of considerable importance. 
 
 YIELD oF Runnina CREEK Tin MINES FROM 1883. 
 
 
 
 1883 ate ay ... 25 tons of stream tin, value ... £1,000 
 1884. ee on rapa’, 5 ae wes 1,134 
 1885 i es RD 3 Pr bee ie 225 
 1886 ee os cceneO. 3 “5 ne re 330 
 
 Total ... — ..» £2,689 
 
 In succeeding years the returns do not admit of the separation of the output of 
 Running Creek from that of Kangaroo Hills. 
 
 ANNAN AND BLOOMFIELD TIN FIELDS. 
 
 These tinfields are comparatively new, and till very recently the only ore 
 exported has been stream tin, which is found in narrow gullies among tropical jungle. 
 Fortunately water is abundant, and washing presents no difficulties. The narrowness 
 of the gullies hitherto worked has made it not worth while to apply hydraulic power to 
 the washing, but this will probably be done in future in the wider and deeper drifts of 
 
11 
 
 the lower reaches of the Annan, Trevethan Creek, and the Bloomfield, where large 
 deposits may be expected to occur. The quantities of ore raised, according to the 
 Annual Reports of the Department of Mines, have been as follow :— 
 
 
 
 
 
 Tons. ; Value. 
 
 1885 ave 300 sie £3,144: 
 1886 wee 148 te 7 400 
 1887 a 945 Nee 58,783 
 1888 fee 1,051 5a 66,949 
 1889 nee 690 ae 38,000 
 1890 Kes 578 atate 34,979 
 Totals)... 3,712 vee £209,255 
 
 The greater part of the above must have been stream tin. From May, 1889, 
 to May, 1890, 540 tons of stone were crushed at the Lion’s Den Machine, yielding 
 49 tons of “black tin.’ The only other machine on the field, that at Mount Browning, 
 only commenced work during the present year (L891). 
 
 The principal lodes occurring in granite or syenite country are the Mount Les- 
 well, Wheal Davey, Collingwood, Lease 96, Cahill Brothers’ Lease, Richmond, Lion’s 
 Den, Mount Hartley, Mount Amos, Mount Browning, Fiery Star, Murray and McArdle’s, 
 Gladstone, and Creighton’s, while Dodd’s Lode and a few others occur in a greywacke 
 rock which may be supposed, like the strata of the Palmer Gold Field, to belong to the 
 Gympie Formation. 
 
 The ore appears to occur in the lodes for the most part in pipes or shoots, 
 associated with quartz, wolfram, and tourmaline, the last sometimes in considerable 
 quantities,* and is occasionally very rich. 
 
 These mines are described in detail in the two reports by the writer. 
 
 CHARTERS TOWERS GOLD FIELD. 
 See Chapter IIT. 
 
 RAVENSWOOD GOLD FIELD. 
 
 The country-rock of this goldfield is a grey syenitic granite, in which hornblende 
 accompanies or takes the place of mica. Actinolite is sometimes substituted for the 
 hornblende. The reefs belong to two distinct systems, one running north and south 
 and underlying to the east, and the other running east and west and underlying to the 
 south. They generally have a quartzose gangue, and contain iron and copper pyrites, 
 arsenical pyrites, zine-blende, galena, &ec., as well as gold. This complex “ mundic,” 
 when exposed to alternate atmospheric and aqueous influences, is decomposed, the 
 metallic compounds being oxidised and the gold set free, and consequently the field was 
 a favourite “poor man’s diggings” till the water level was reached. At that level, 
 however, the majority of the mines suffered a severe check, as it was found to be 
 impossible to save more than a small proportion of the gold by amalgamation. The 
 products of some of the richer mines were for a time sent to Europe for treatment, but 
 many of the others which had paid well in the “ brownstone” did not produce a sufficient 
 quantity of rich ore to yield a profit after paying expenses, of which the carriage to the 
 coast formed the heaviest item. Roasting was also resorted to, and was successful in some 
 cases. Smelting was next tried, but proved too costly. Chlorination and the “Cyanide” 
 ‘ process have also been tested. Improvements in these processes will probably ere long 
 prove equal to the extraction of the gold from what has hitherto been found an unusually 
 refractory ore, when Ravenswood will take high rank among Australian goldfields. 
 
 
 
 
 
 * See Mr. Clarke’s Petrographical Notes. 
 + Geological Observations on the North of Queensland, 1887; and Second Report on the Tin Mines 
 near Cooktown, 1891. : 
 
12 
 A considerable quantity of alluvial gold has been obtained in Elphinstone Creek 
 and other streams on the field, mainly by Chinese, who turn over the wash again and 
 again. Alluvial and reef gold have, however, not been distinguished in the early returns, 
 and in more recent years part of the gold in the alluvial may have been derived from 
 
 tailings. 
 YIELD oF RAVENSWOOD GoLp FIELD. 
 
 
 
 
 
 
 
 
 
 
 
 REEF GOLD. 
 Year. Seip &., Total Gold. Remarks, 
 ST 8 oath 
 To end of — | Oz. Oz. 
 
 1875 ae vad eo 170,649 | Deduced from figures in Report 
 Department of Mines for 1884, 
 p. 10 
 
 1876 oY “se Ay 18,788 | Includes gold from pyrites and 
 tailings 
 
 1877 10,441 11,963? a 11,963 
 
 1878 15,500 13,2521 aes 13,252 | 1 Includes gold from pyrites and 
 
 1879 15,700 15,7442 me 15,744 tailings 
 
 1880 13,479 12,6201 825 13,445 
 
 1881 10,880 8,600? 2,5953 10,195 | ? Includes gold from tailings 
 
 1882 7,854 5,002 3,7094 8,711 
 
 1883 7,985 6,054: 6,946 13,000 | *% Includes gold from exported 
 
 1884. 13,202 11,828 2,3645 14,192 mundic 
 
 1885 11,039 15,916 1,7255 17,641 
 
 1886 4,706 7,406 1,8395 9,245 | * Includes alluvial gold and gold 
 
 1887 6,589 6,842 38,0485 10,390 from tailings and exported 
 
 1888 11,560 8,875 IAS? 10,666 mundic 
 
 1889 19,498 14,600 1,119 15,719 
 
 1890 17,796 14,731 1,822 16,053 | > Classed as “alluvial”? by warden 
 
 otal meee Ate 369,653 
 
 
 
 RAVENSWOOD SILVER FIELD. 
 
 A belt of argentiferous rocks extends for about six miles north-westward from 
 the richest part of the Ravenswood Gold Field. Although the goldfield and the silverfield 
 are both in granite country, a tolerably distinct line may be drawn between the grey 
 syenitic granite of the goldfield and the coarse-grained red granite of the silverfield. 
 The latter is a mixture of roundish blebs of quartz, flesh-coloured or pinkish orthoclase 
 crystals, and hexagonal mica. The principal lode, known as King’s, or the One-Mile, 
 runs N. 28° W., and underlies at 35° to H. 28° N. It is a very rich lode, and frequently 
 consists of two parallel veins. The surface yielded carbonates of lead, giving as much 
 as 300 oz. of silver to the ton. The lower levels have given a steady yield of galena ores, 
 with, as a rule, 2 oz. of silver per ton to the unit of lead. The galena is in places a 
 good deal mixed with pyrites and zine-blende. In a shaft in Lease 109 the lode has been 
 cut at a vertical depth of 650 feet. The shaft bottomed on an antimony and copper ore, 
 somewhat resembling tetrahedrite in its composition, but containing from 500 oz. to 
 5,000 oz. of silver to the ton. Pumping and winding and dressing machinery were 
 erected to work this rich deposit, which, however, appears to have thinned out. 
 
 The Mount Right Lodes, at the north-western end of the argentiferous belt, 
 have not yet been worked on a large scale, although the Warden reported that in 1883 
 a single miner raised 20 tons of galena ore, worth £400. In 1884 the same “hatter” 
 raised 26 tons, worth £702. Some thin lodes of antimony ore occur among the’ silver- 
 lead mines of Mount Right. 
 
13 
 
 In the following table, the great bulk of the ore has been raised from King’s 
 Mine. The other mines are specified where the information is given in the Annual 
 Reports of the Department of Mines. 
 
 YIELD OF RAVENSWOOD SItVER FIELD. 
 
 
 
 
 
 
 
 
 
 
 
 Year, | Mine. Tons ef Ore. ee ae cr Value. 
 Ah uh 
 1880 43 Mount Right ... gaa 124 Exported 371 5 O 
 ” 44. r nee ae 25 9 86 1 3 
 ” One-Mile (King’s ?) ae 108 es 3,152 10 0 
 1881 Kinder oer asa Os: 357 iG 14,040 0 0 
 5p Roberts and Others Me 20 Fe 1,400 0 O 
 1882 not 2003 9 6,762 0 O 
 1883 an 381 A 12,072 0 O 
 1884 “6n 895 a 20,560 0 O 
 1885 sia 905 F) 22,937 O O 
 1886 cae 928 Dressed 23,114 0 0 
 1887 nae 1,142 Raised 25,520 O O 
 1888 wAC 11 ne 140 0 O 
 
 1889 7 Ae 500 nt 
 
 1890 King’s Ae si aa 2743 Raised 6,411 17 6 
 Totals ... 506 Bi 5,2314 ses 136,566 13 9 
 
 
 
 SELLHEIM BISMUTH MINES. 
 
 Three miles east of the township of Eukalunda, on the north side of the Mount 
 Wyatt and Bowen road, is the Daisy Bismuth Mine. The cap is traceable for one chain 
 E. 20° N. to a shaft 12 feet deep. In the shaft the lode is at least 3 feet 4 inches 
 wide, for neither hanging nor foot wall is seen. It has an 8-inch vein of iron and 
 copper ore with greenish-yellow imperfect prismatic crystals of bismuth ore. The 
 vein underlies at a high angle to S. 20° E. Horizontal veins of ore go into both sides 
 of the shaft. The matrix of the ore is mainly red iron oxide with a considerable 
 proportion of “tile ore,’ or ferruginous red oxide of copper. It contains some 
 green and blue carbonate of copper, sometimes in crystals, and a considerable quantity 
 of the bismuth ore already mentioned. The greenish-yellow crystals yield bismuth, 
 copper, and iron, the bismuth and copper being in the condition of carbonates. It is 
 probable that the ore results from the transmutation of wittichenite or cupreous 
 sulphate of bismuth, which will probably take its place (mixed with iron and copper 
 pyrites) below the water level. It may be mentioned that wittichenite is steel-grey to 
 white in colour, has a black streak, tarnishes pale lead-grey, and contains about 48 per 
 cent. of bismuth and about 33 per cent. of copper. A sample of the greenish-yellow 
 bismuth ore freed from the matrix gave me on analysis 33°76 per cent. of bismuth. 
 
 A hole just being sunk 100 yards to EH. 20° N. shows ore 2 feet 8 inches in width, 
 mostly iron, manganese, and copper oxides, with some green copper carbonate, and some 
 lumps of yellow bismuth ochre. Another pothole, one chain further along the cap, 
 shows specks of galena, and heavy iron, copper, and manganese oxides. It was opened 
 some years ago by prospectors for silver. The country-rock is syenite. 
 
 Half-a-mile east of the Daisy is the Eukalunda Bismuth Mine. It commences 
 at the south-west end with a very large blow (say 12 feet wide) of red ironstone, with 
 some manganese oxide, quartz, and streaks and spots of greenish-yellow bismuth ore. 
 A hole 12 feet deep shows it to underlie at a high angle to the south-east. A shaft 
 20 feet deep about 40 feet to the north-east shows the same underlie, but does not prove 
 the width of the lode. The shaft shows ferruginous quartz with some bismuth ochre, 
 
14 
 
 traversed by horizontal yellow clay veins. One chain further north-east a shaft 40 feet 
 deep shows.the underlie of the lode to be 80°. The ore is to a large extent composed of 
 yellow oxides of bismuth and iron, red iron oxide, some copper pyrites, and large 
 quantities of greenish-yellow bismuth ore. The lode is at least 5 feet wide, but the 
 hanging-wall is not seen in the shaft. There are two veins of ore, each about 10 inches 
 thick, and veins of ironstone run towards the hanging-wall side of the shaft at an angle 
 of 45°. For about 8 chains north-east of the 40-feet shaft the greenish-yellow bismuth 
 ore is traceable in the cap of the lode. For 7 chains further only ironstone is seen.* 
 
 The Reports of the Department of Mines show the output for the last two years 
 to be as follows, the mines having as yet been only worked on an experimental scale, 
 owing, I believe, to the difficulty in getting access to the bismuth market :— 
 
 Ore Raised. Estimated 
 Tons. Value. 
 1889 wae es nae 44, a £8,300 
 1890 yee bee Sah 6 eae 681 
 
 CROYDON GOLD FIELD. 
 
 This goldfield was only discovered in the end of 1884, and for some time its 
 importance was not recognised. After some extraordinary crushings of Croydon stone 
 at the Etheridge the first machine was opened on the field in November, 1886, and since 
 then the prosperity of the place has advanced rapidly. The population was estimated 
 at 8,000 in December, 1887, and (by the Warden) at 3,212 in December, 1889; the 
 floating population attracted by the first rush having been reduced to the number neces- 
 sary for the industry. The township is now connected by rail with Normanton. 
 
 The part of the field immediately surrounding the township lies in a hornblendic 
 granite, but north and east of the town is a wide-spread rock, apparently of metamorphic 
 origin. It has a flinty ground-mass, and shows at one end of the series a clastic structure 
 like an altered conglomerate, and at the other fluxion-structure.+ Many of the reefs lie 
 rather flat, and this circumstance gave rise at first to misgivings as to their permanency ; 
 but this prejudice, like many others, has had to yield to the logic of facts. In some the 
 gold is very much alloyed with silver. One line of reef shows a good deal of native silver. 
 
 The township is on the very edge of an alluvial flat which extends to the Gulf of 
 Carpentaria. Of some of the deposits in this flat it is impossible to say whether they are 
 recent alluvial “cements” or belong to the Desert Sandstone. The auriferous rocks them- 
 selves nowhere rise to any considerable elevation, and are overlaid in places by isolated 
 fragments of fossiliferous Desert Sandstone, which are alluded to in another place. 
 
 Besides the township of Croydon proper, Carron, Golden Valley, Tabletop, 
 Goldstone, The Homeward Bound, The Mark Twain, The Croydon King, The Springs, 
 and Wallabadah are centres of mining industry in the neighbourhood. 
 
 YIELD oF Croypon Gotp FIELD. 
 
 
 
 
 
 
 
 
 
 Year. Stone Crushed. | Yield therefrom. Alluvial Gold. Total Gold. Average Value of Gold per oz. 
 Tons. Oz. is Same Oz. 
 1887 10,950 31,787 (Not estimated) 31,787 £2 13 6 (Local value) 
 1888 22,792 44,839 23 oz. 44,862 £217 3% (Mint value) 
 1889 29,439 52,541 (Not estimated) 52,541 £2 11 4% (Local value) 
 1890 43,226 60,368 (Not estimated) 60,368 £2 13 3 (Local value) 
 Nota jens An 189,558 
 
 
 
 * Report by R.L.J. on the Sellheim Silver Mines and Surrounding District. Brisbane: 
 Authority : 1889, 
 
 + See Mr, Clarke’s Notes. 
 
15 
 
 ETHERIDGE GOLD FIELD. 
 
 The greater part of this extensive field is a coarse-grained granite with large 
 erystals of orthoclase felspar and flakes of mica.* Of this granite Mr. Daintree 
 remarkst that it is simply transmuted mica schist, as shown by the presence of 
 occasional bands of unaltered schist throughout the mass. The principal drawbacks to 
 the field hitherto have been its inaccessibility and the isolated position of the reefs. 
 Mines, without an output sufficiently large to keep their own crushing machinery going, 
 have again and again been abandoned owing to the cost of carriage to the nearest Snail 
 The principal centres of mining are the Cumberland, Durham, Georgetown, Finnegan’s, 
 and Goldsmith’s 
 
 The Cumberland Mine, which has been one of the most productive on the field, 
 has an elvan dyke between the walls, the reef sometimes occupying its upper and 
 sometimes its lower side. The quartz reefs, except above the water level, are generally 
 charged with iron pyrites, copper pyrites, arsenical pyrites, zinc-blende, and galena, in 
 varying quantities. The mines at Goldsmith’s form, geologically, part of the Gilbert 
 Gold Field, being situated in mica-schist country, although geographically they belong 
 to the Etheridge Basin. The stone from these mines is less difficult to treat than that 
 from the reefs in the granite. 
 
 The Etheridge and Gilbert having been, during the greater part of their history, 
 in charge of the same Warden, the returns from these fields have been generally 
 lumped,together. This is unfortunate for statistical purposes, as the two fields are 
 geologically distinct. In the following table the greater part of the reef gold must 
 have come from the Etheridge, and the greater part of the alluvial gold from the 
 Gilbert. In 1881 and 1882 the return also includes gold from the Woolgar. The 
 amount from the Woolgar in 1881 must have been trifling, as the Warden at the end of 
 the year reported that the crushing machinery was only “ nearly ready.’ In 1882 the 
 amount from the Woolgar was probably about 2,000 oz. 
 
 YIELD OF ETHERIDGE GoLD FIELD. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 Year. Stone Crushed. Yield therefrom. Alluvial Gold. Total, 
 To end of— Tons. Oz. 02 Oz. 
 
 1875 in a - $129,798 
 1876 Kate ned Sot 13,202 
 1877 3,134 4,837 ate 4,837 
 1878 3,550 6,365 1,031 7,396 
 1879 4,417 5,927 9,571? 15,498 
 1880 4,455 8,821 11,547 20,3868 
 1881 12,151 20,926 2,104: 23,030 
 1882 7,428 13,190 5,241 18,431 
 1883 10,751 16,127 2,840 18,967 
 1884. 7,010 | 16,560 1,000 17,560 
 1885 11,354 22,708 eee 22,708 
 1886 10,983 22,700 500 23,200 
 1887 8,100 24,603 50 24,653 
 1888 § 8,606 § 22,662 ee 22,662 
 1889 \| 11,083 || 18,150 AY 18,150 
 1890 18,575 || 24,310 270 24,580 
 Total ... AY 405,040 
 
 
 
 * See Mr. Clarke’s Notes. 
 
 + General Report upon the Northern District. Brisbane: by Authority : 1870. 
 
 + Deduced from figures in Report of the Department of Mines for 1884, p. 11. 
 
 § Including Woolgar, but excluding Mount Hogan, which is added to Gilbert returns. 
 || Including Woolgar, Mount Hogan, and Gilbert. At these places little appears to have been done, 
 
16 
 
 EIDSVOLD GOLD FIELD. 
 
 “The country-rock round about Eidsvold consists of granite, which for the most 
 part is medium-grained, of a pinkish-brown colour. Its constituents are orthoclase 
 felspar, largish blebs of quartz, and small crystals of mica (biotite). The rock passes 
 in parts into a fine-grained syenitic granite of a darkish colour, and contains hornblende 
 in addition to mica. 
 
 “The reefs are situated in the granite country. They are running in various 
 directions, though the majority of them have a north-west to north-north-west bearing. 
 They lie very flatly in most cases, the underlie varying from 45° to 75°. 
 
 “All the reefs contain a certain amount of mundic; and, as the water level has 
 not yet been reached, the quartz is often of an ochreous or gossany nature from the 
 decomposition of the sulphurets. It is probable that the reefs will be rich in sulphurets 
 at a depth. 
 
 “ Eidsvold, in many respects, somewhat resembles the Charters Towers Gold 
 Field. The chief points of resemblance are—the country-rock, which in both places 
 consists to a great extent of granite and syenite or syenitic granite; in the flat underlie 
 of the reefs; and in the character of the gangue of the reefs, which consists in both 
 places, to a great extent, of decomposed granite débris with veins of quartz. 
 
 “Comparatively small amounts of the sulphurets (pyrites and galena, &c.) have 
 yet been met with in the Eidsvold reefs, owing, no doubt, to the fact that the workings 
 have not yet reached beyond the action of atmospheric influences. The quartz, however, 
 is often ferruginous, and contains a yellow ochreous material which has been produced 
 by the decomposition of these sulphurets, which will be found to exist in large quantities 
 in the reefs when the water level is reached. A few of the reefs contain a good per- 
 centage of galena, a mineral of very common occurrence in the Charters Towers reefs. 
 Very little copper ore occurs in the reefs. On the other hand, arsenical pyrites is of 
 common occurrence here in some reefs. I did not meet with any zine ore at Eidsvold, 
 while sphalerite (zine-blende) is of common occurrence at the Towers. 
 
 “The field, as far as can be gathered from surface indications, is, with the 
 exception of a few porphyry and syenite dykes, singularly free from eruptive dykes. 
 
 “So far as can be judged from the work already done, the prospects of Hidsvold 
 as a reefing district are very good. 
 
 “The field will soon have the advantage of a thorough trial, for two or three 
 batteries will soon be on the field.” (Report on the Hidsvold Gold Field, by William 
 H. Rands, Assistant Government Geologist.) 
 
 In the report above quoted, Mr. Rands gives detailed descriptions of the several 
 reefs, and mentions the occurrence of tin ore (cassiterite) in one of them, associated 
 with tourmaline, and of stibnite (sulphide of antimony) in another. 
 
 YIELD OF ErpsvoLD Gorp FIELD. 
 
 
 
 
 
 
 
 REEF GOLD, 
 Year. ee ee SS ee ee ee ee | Alluvial Gold. Total Gold. 
 Stone Crushed. Gold therefrom. 
 Tons. Oz. Oz. Oz. 
 LSS 7aer aie ee at 27 84 i 84 - 
 1888 ... sk See oa 7,768 6,907 100 7,007 
 1889 ... ee ie oe 15,933 15,446 150 15,596 
 TSSOiee ane ree at 20,910 15,823 110 15,933 
 Totals wh 44,638 38,260 360 38,620 
 
r7 
 
 MOUNT PERRY COPPER MINE. 
 
 Although this is not the only copper-mine in the district, it is the only one 
 which has been worked continuously and on a large scale. 
 
 Mr. Israel Bennett, Inspector of Mines, and formerly manager at Mount Perry, 
 was good enough to give me the following notes in 1885 :— 
 
 “Seven shafts have been put down on the lode to various depths; the main or 
 engine shaft is now between 800 and 900 feet deep. The course of the lode is 
 N. 37° E., and where it is at present being worked (to the south-west of the main 
 shaft) it hades to the south-east about 8°” [from the vertical]. ‘‘ Near the surface 
 the ore consisted of green carbonate and azurite, and at 30 feet deep of rich red 
 (cuprite) and grey oxides of copper, and below this depth of yellow ore and copper 
 pyrites. The pyrites is contained in a veinstone of quartz and calcite, each of which 
 predominates in turns. To the north of the main shaft much iron pyrites has been met 
 with mixed with the copper ore. At the present depth [1885] the lode is about 4 feet 
 in width. The width of ore is about 10 inches on an average.” . . . ‘ There are 
 numerous cross-courses, which, although they do not displace the lode, yet often affect 
 the ore in the lode, either by breaking it up into strings, or by displacing it from one 
 side of the lode to the other. At these points of intersection the lode is usually 
 enriched. A dyke of orthoclase porphyry runs parallel with the lode, and is displaced, 
 too, by the cross-courses. Two dykes of dolerite also cross the lode in a north-westerly 
 direction.” 
 
 The country-rock is a syenitic granite which Mr. Rands regards as metamorphic. 
 The granite in places has carbonate of copper disseminated through its mass. At the 
 Queensland Claim, the granite is worked as a low-percentage ore (10 per cent. of 
 copper) to assist in the smelting of the pyrites at the Mount Perry Mine. 
 
 The output of the mine prior to 1885, according to Mr. Bennett, was— 
 
 
 
 
 
 95 tons ore at £20 ... sae creel OOO MOS: 
 19# Re ALD pani 3 is 197 10s. 
 1,200 tons copper at £70... nae ... 84,000 Os. 
 Total age ».. £86,097 10s. 
 
 In 1888 the Annual Report of the Department of Mines shows 1,096 tons of 
 copper ore, valued at £9,128, and in 1889, 978 tons of copper ore, valued at £10,000, 
 from the Tenningering District. This was probably for the most part the product of 
 the Mount Perry Mine. In 1890 the amount of copper raised in the Tenningering 
 District was 85 tons, valued at £1,000, and the Mineral Lands Commissioner reports 
 the Mount Perry Mine to have been closed. 
 
 The Canterbury and Normanby Lodes_ adjoin and run parallel with the Mount 
 Perry Lode. Nine miles to the west is the Potosi Lode. It contains galena, with copper 
 and iron pyrites and a little zinc-blende, in a gangue of quartz and barytes. The 
 Mungai Lodes are three miles further west, in a country-rock of actinolite schist. From 
 these lodes carbonates of copper are raised for smelting with the Mount Perry ores. 
 
 The Wolca Lodes are six miles north of Mount Perry. Some of these contain 
 gold, one (the Allendale) as much as 15 dwt. to the ton, as well as copper ore. There 
 is another group of lodes in the paddock of Wombah Station. 
 
 The Boolboonda Mines lie to the east of the granite country, in a belt of 
 metamorphic rocks, consisting of gneisses, schists, quartzites, &c. The Boolboonda, 
 Cambria, and New Moonta Lodes contain gold as well as copper—apparently in several 
 cases in proportions which would be payable under favourable conditions.* 
 
 * For further details see Mr. Rands’ Report on the Gold Fields of Raglan, &c., and the Mineral 
 
 Deposits in the Burnett District. Brisbane: by Authority: 1885, 
 B 
 
18 
 
 TENNINGERING, BOOLBOONDA, MOLANGUL, AND NORMANBY GOLD FIELDS. 
 
 The Reid’s Creek reefs are about five miles south-south-west of Mount Perry, 
 on Branch Creek, a tributary of Reid’s Creek. These, reefs, Mr. Israel Bennett, 
 Inspector of Mines, informs me, have turned out, up to 1886 (I gather from the 
 Annual Reports of the Department that they have only been worked since 1881), 400 
 tons of stone, valued at £15 per ton, £6,000, and 1,200 oz. of gold, valued at £3 10s. 
 per oz., £4,200 ; total, £10,200. At a depth the lodes yield a mundic consisting 
 chiefly of arsenical iron pyrites, but containing also iron pyrites and zinc-blende, with 
 here and there blocks of galena. 
 
 None of the other smaller fields in the Burnett District have ever attained to 
 much importance, and it would be impossible to estimate their yield with any degree of 
 accuracy. They are grouped together in the official returns, sometimes under one 
 heading and sometimes under another. The little field which produced all the gold in 
 one year’s return was perhaps abandoned the next, so that the gold-mines of the whole 
 Burnett District have to be regarded as one group. Probably even thus the returns are 
 unsatisfactory. For instance, Mr. Rands in his Report, published in 1885, gives the 
 output for 1884 of the Reid’s Creek mines alone as 688 oz. of gold from 830 tons of 
 stone, while the output of the whole district for the year is given in the Annual Report 
 of the Department of Mines as 431 oz. from 603 tons. 
 
 YIELD OF TENNINGERING AND OTHER SMALL GOLDFIELDS IN BuRNETT DISTRICT. 
 
 
 
 Year. Stone Crushed, Gold therefrom. Total Gold. 
 Tons. Oz. Oz. 
 
 LSSORE.. ae Nes 500 Nee ans 63 
 Issive ee a of 1,809 1,254 1,254 
 SS Zee siete sae se 889 622 622 
 i'SS3 eee. ae are ah 355 376 376 
 1884 ,.. cane Aa oa 603 431 431 
 LSS Sars See its ay 127 92 92 
 USS Oecs see oe ae 1,066 : 90 90 
 188faeee ee obs ” 1,398 671 671 
 AS88ie tise nite sare a 2,428 ; 1,553 * 1,553 
 SSO can dae Aas 2,085 1,246 1,246 
 PSO ues as as Aae 2,341 1,901 1,901 
 
 TV otalars an 8,299 
 
 
 
 
 
 JIMNA AND GOOROOMJAM GOLD FIELDS. 
 
 Jimna Gold Field has been worked off and on for more than twenty years, but has 
 not been highly productive, except at first, for alluvial gold. Its output, when reported, 
 has generally been massed in the annual returns with those of “ Other Small Fields.” 
 
 The rocks at the Jimna Diggings are principally granite, slate, and sandstone, with 
 comparatively little quartz. The alluvial drift of the only two creeks that have been 
 worked—Jimna and Sandy Creeks—rests sometimes on decomposed granite and some- 
 times on sandstone or slate. The workings have extended four or five miles down each 
 of these creeks. Mortimore’s reef, on Jimna Creek, contains fine gold. It is interesting 
 as having been the first auriferous reef observed in the colonies traversing granite 
 country. 
 
 J. 
 
 
 
CHAPTER III. 
 
 METAMORPHIC ROCKS (SLATES, SCHISTS, GNEISSES, &c.) OF 
 UNDETERMINED AGE. 
 
 Mineral Areas—viz., Cloncurry Gold and Copper Fields, McKinlay Gold Field, Charters Towers 
 and Cape Gold Fields, Gilbert and Woolgar Gold Fields, Coen Gold Field, Normanby and 
 Marengo Gold Fields, Peak Downs Gold Field, Peak Downs Copper Field. 
 
 Aurnovuen the area of metamorphic rocks, of which the age had not been deter- 
 mined when I issued my Geological Map of the Colony in 1886, has been considerably 
 reduced in the present edition, it will be seen that a considerable area still remains. 
 
 In 1872 Mr. R. Etheridge, F.R.S., stated* that the Broken River limestones 
 _ (Middle Devonian), which he called ‘ Siluro-Devonian,” were the lowest fossiliferous 
 rocks in Queensland. The late Rev. W. B. Clarke (I think, erroneously) ascribed to 
 Mr. Etheridge the view that “ nothing lower than Siluro-Devonian rock has been found 
 in Queensland.” No older fossils have yet been discovered, but lower and older stratified 
 rocks certainly exist. 
 
 The granites and syenites of Charters Towers:appear to be the ultimate stage in 
 the metamorphism of the series of stratified rocks described in my Report “ On the 
 Geology and Mineral Resources of the District between Charters Towers Gold Field 
 and the Coast.’’+ 
 
 These rocks are older than the Burdekin Beds. They are all metamorphosed in 
 a greater or less degree. The metamorphism must have taken place prior to the deposi- 
 tion of the Burdekin Beds, pebbles and granules of the metamorphosed rocks forming 
 the material of which the conglomerates of-the latter series are built up. 
 
 These once horizontal beds are now thrown into broad folds, and probably do not 
 occupy more than one-fourth of the surface over which they were deposited. The 
 stratified rocks occur to the north and west of Charters Towers. They consist of 
 quartzites, slates, and shales. The slates do not differ from the shales in mineral 
 composition—mainly silicate of alumina, with a high percentage of peroxide of iron— 
 but simply in being intersected by cleavage planes. Both the slates and the greywackes 
 are, as a rule, highly impregnated with iron, being in places “iron-masked” to such a 
 degree that they might almost be taken for weathered clay-band ironstones. 
 Occasionally, where the greywackes are fresh and contain little iron, they somewhat 
 resemble blue limestone, while their joint-surfaces are often coated with cale-spar. A 
 conglomerate of small quartz-pebbles, enclosed in a matrix of fine sandstone (mainly of 
 felspathie materials), coloured dark red with peroxide of iron, is met with in two places 
 between Charters Towers and the Burdekin. In these stratified rocks no fossils have 
 as yet been detected. 
 
 Again, in the valley of the Reid, the Middle Devonian limestones rest unconform- 
 ably on greywackes, &c., which are probably of the same age as the stratified rocks west 
 of Charters Towers, and have interstratified with them some thick beds of brecciated 
 
 voleanic ash. 
 
 
 
 * Quart. Journ. Geol. Soc., vol. xxviii., p 384, 
 + Brisbane: by Authority: 1879 p. 15, 
 
20 
 
 In the neighbourhood of Clermont a series of gold and copper-bearing schists, 
 slates, quartzites, &c., is apparently overlaid unconformably by a bed of limestone of 
 Devonian age. * 
 
 In many other localities, stratified rocks, belonging to formations newer than the 
 Devonian, rest unconformably on upturned strata which are more or less metamorphosed, 
 but, beyond the superposition of the newer formations referred to, there is nothing to 
 indicate the age of the upturned rocks in the absence of paleontological evidence. 
 
 The whole of the strata classed as ‘‘ undetermined,” consisting originally of lime- 
 stones, conglomerates, siliceous and felspathic sandstones, clay shales and mudstones, 
 are generally thrown into sharp folds, and are often locally metamorphosed into marbles, 
 quartzites, greywackes, mica- and talc-schists, lydian stone, &c.; or, still further, to 
 the utter obliteration of their originally stratified character, into serpentines, diorites, 
 hornblende- and tourmaline-gneisses, porphyries, granites, &c. 
 
 In succeeding chapters it will be seen that Daintree and other geologists ascribed 
 large areas of these metamorphic rocks to the Silurian and Devonian, chiefly on the 
 ground of their lithological resemblance to the strata of these formations as developed 
 in Victoria and New South Wales. In regions so far distant I cannot attach any 
 importance whatever to evidence of this nature. 
 
 It is impossible to hazard even a guess as to the total thickness of the meta- 
 morphosed strata on which “no name” has been inscribed. Mr. Rands estimatest the 
 thickness of the metamorphic schists and quartzites of the Cape Gold Field alone at 
 from five and a-half to six miles. 
 
 It is to be hoped that all thé rocks now mapped as “of undetermined age” will 
 be relegated to their proper horizons by future observers, and it is more than likely that 
 the greater portion wiil be distributed between the Permo-Carboniferous and Devonian. 
 Possibly representatives of some of the older Palzozoic formations which, so far as we 
 know, are absent from Queensland, may yet be detected among the more or less meta- 
 morphosed strata. It may be suspected that the limited areas of metamorphic rocks in 
 the south-western corner of the Colony are a prolongation of the Cambrian rocks of 
 South Australia and the north-western portion of New South Wales. 
 
 We have not as yet been able to recognise in Queensland by direct evidence any 
 equivalents for the Cambrian of Yorke’s Peninsula, South Australia, nor for the 
 Graptolite-schists of. Victoria, nor for the Upper Silurian limestones of Yass and 
 Bowning, New South Wales, and of Lancefield, &c., and the Upper Yarra Basin in 
 Victoria. 
 
 It would be beyond the scope of this work to attempt to give a detailed descrip- 
 tion of the metamorphic rocks of Queensland. Such descriptions will be found in 
 overwhelming detail in the voluminous writings of Stutchbury, Aplin, Daintree, 
 Gregory, and the officers of the present Geological Survey. 
 
 MINES IN CONNECTION WITH METAMORPHIC ROCKS OF 
 UNDETERMINED AGE. 
 CLONCURRY GOLD AND COPPER FIELDS AND McKINLAY GOLD FIELD. 
 The greater part of this extensive area is covered by highly inclined slates, 
 quartzites, and greywackes, with occasionally a bed of limestone. These have so far 
 proved unfossiliferous, and there is no distinct evidence of theirage. These rocks form, 
 
 
 
 * Report on the Geology and Mineral Deposits of the Country in the Vicinity of Clermont. Wo. 
 Rands. Brisbane: by Authority: 1886. See also Chapter VIII. 
 + Report on the Cape River Gold Field. Brisbane: by Authority; 1891. 
 t Is it possible that some of these beds of undetermined age may also represent the Azoic rocks of 
 South ‘Australia, below the Cambrian ?—R.£, jun”. 
 

 
 21 
 
 as it were, a peninsula extending south-eastward from the north-west corner of the 
 Colony, and projecting into the Cretaceous rocks of the Rolling Downs Formation. 
 In the neighbourhood of the Mount Douglas gold-mines the country is studded with 
 rugged knobs of granular quartzite, which may represent the discharge pipes of thermal 
 springs. The field is intersected with enormous siliceous veins like those of the 
 Hodgkinson Gold Field. A few small isolated tablelands of the Desert Sandstone 
 attest the former extension of that formation. 
 
 The gold-mines have been worked in a desultory and unsatisfactory manner, for 
 which the position of the field is no doubt in large measure to blame. The Gilded Rose, 
 on Fisher’s Creek, in a country-rock of flaggy taleose sandstones and shales, has been 
 most persistently worked. The reef is highly charged with pyrites. The carbonates of 
 copper in the Homeward Bound and Flying Dutchman lodes contain a good deal of 
 gold. In the Uncle Tom, on Pumpkin Gully, the gold is associated with quartz, 
 carbonate of lime, and carbonate of iron. In the Mary Douglas, at the Top Camp, 
 rich deposits of gold, associated with native bismuth, have been obtained from quartz 
 coated with botryoidal and stalagmitic masses of glossy-black limonite. Within the last 
 few weeks, much excitement has been created by the discovery of the Last Call Mine, 
 near the Soldier’s Cap (a Desert Sandstone tableland), to which the Goldfield Warden 
 refers as follows, in a Report to the Minister for Mines, published in the Brisbane 
 Courier * :— 
 
 “On two occasions I visited the mine and found by careful tests the whole body 
 of conglomerate extremely rich, the prospects I took giving on my first inspection from 
 5 oz. to 12 oz. from the heap at grass and in the lower workings in bottom of shaft, and 
 in the faces of the drives and crosscuts overhead, and at foot the prospects were really 
 splendid. Assays made from stone taken from a leader running through the great bulk 
 of the deposit gave startling results—far too good to anticipate anything equal in the 
 average of any mine yet found. The main body of this singular deposit is a granular 
 carbonate of lime with a considerable proportion of micaceous sandstone and some oxide 
 of iron (miners’ black sand). The largest of the gold consists of fine hair-like threads, 
 not exceeding half-an-inch in length, diminishing in size to the smallest speck of dust. 
 A quantity of specular and red hematite iron ore is also obtained, carrying a large 
 percentage of gold similar in quality to that in the limestone, but the thread filaments 
 are absent. The area of the lease is 6 acres, and although considerable preliminary 
 work has been necessary, such as sinking wells, timbering, road-making, &c., good 
 progress has been made in the mine. The shaft has been sunk 38 feet, and drives put 
 in north and west, and about 100 tons of crushing stuff paddocked. With a view to 
 test the capabilities of their property, the owners purpose sending a few tons to the 
 machine at Soldier’s Cap, and probably 2 tons will shortly be in transit to Charters 
 Towers for treatment. Two indeperdent tests from bulk made in Sydney gave over 
 38 oz. of gold and nearly 8 oz. of silver, and one in Charters Towers, in which no gold 
 was visible, gave 69 oz. gold and nearly 12 oz. silver. From the leader before mentioned 
 2 lb. weight of stone when reduced yielded 1 oz. of excessively fine gold. The various 
 leases adjoining No. 15 have struck nothing as yet; but at greater depth I consider 
 Nos. 17 and 21, on the south, and No. 18, on the west, the best properties, although it is 
 difficult to predict where the run may extend, as the whole of Martin’s Creek formation 
 presents something unique in mining, and is certainly puzzling to the devotees of old 
 mining legends.”’ 
 
 The gullies and flats radiating from the Mary Douglas Hill have yielded rich 
 alluvial gold, all heavy and nuggetty, and frequently so coated with iron oxides that the 
 
 
 
 * 3rd June, 1891, 
 
22 
 
 miners knew it a8 “black gold.” One nugget weighed 28 lb. Alluvial gold, with 
 native bismuth, is’extensively distributed in the Pumpkin Gully region, and would pay 
 well to work by hydraulic power, if that could be brought to bear on it. 
 
 The total amount of alluvial gold reported since 1877 is 4,751 oz., but it is 
 obvious that the returns are very incomplete. The total amount of reef gold from 1877 
 to 1890 is 5,288 oz., but, as the amount of stone crushed is not in all cases given, the 
 yield per ton cannot now be estimated. 
 
 The McKinlay Gold Field is believed by many to be a promising one, but has 
 not as yet been steadily worked. Several reefs have given good returns for a time, 
 and a considerable quantity of alluvial gold has been won, but no record appears to have 
 been kept. The country-rock is said by Daintree to be of metamorphic rocks (gneiss 
 and mica- and talc-schists). ‘‘ The associated minerals ave gold and copper, the presence 
 of ‘dykes’ of intrusive material seeming to be the chief cause of mineralisation.”’* . 
 
 YIELD OF CLoncuRRY GoLp FIELD. 
 
 
 
 
 
 
 
 
 
 Year. Stone Crushed. Yield therefrom. Alluvial Gold. Total. 
 
 Tons. Oz. Gold. Oz. Oz. 
 1877 Ae, ae ce 1,190 1,205 alluvial ? 295 1,500 
 1878 ate re a 1,014 1,316 Meds Fe. 1,316 
 1879 ah ies ae 209 293 ae 293 
 1880 ah Mae A 406 490 oe 490 
 
 1881 Ea ats 3B sr no returns a aor 
 1882 she sis af. 410 453 oe 453 
 1883 7A pe aes no returns say 500 say 500 1,000 
 
 1884 oat sia Pers no returns no returns aoe ar 
 1885 aN 3 Bs no returns 50 alluvial ? 400 450 
 1886 Asie Sas San 80 85 566 651 
 1887 male i ee wae see 1,262 1,262 
 1888 we ia a sere a 402 402 
 1889 ik Be ve 1,600 836 410 1,246 
 1890 dis Pe Ap 318 55 736 791 
 Total ,.. end Ree 9,854. 
 
 
 
 The Cloncurry Field contains some very extensive deposits of copper ore. The 
 chief of these are the Great Australian and the Argylla. The copper is in the form of 
 carbonates and red oxides. The latter ore, of which there are enormous deposits, is 
 frequently richer than chemically pure red oxide, being mixed up with native copper. 
 The Great Australian is the only mine which has yet been worked to any extent, and 
 has produced, in 1885-7, 3,250 tons of ore, valued at £33,520. 
 
 YIELD OF CLONCURRY CoPpPER FIELD. 
 
 
 
 
 
 1885 ize 1,340 tons raised = Value, £18,920 
 1886... 900, a - 7,000 
 1857 eee O10 Gea & "i 7,600 
 
 Totals .., 3,250 tons £33,520 
 
 Argentiferous lead lodes occur on the field, chiefly in the Dugald Valley. One 
 of these, still unworked, is over a mile in length. 
 
 The most striking features of the country are mountains of pure specular and 
 magnetic iron ore. One of these—Mount Leviathan—is about two hundred feet high, 
 and a quarter of a mile in diameter at its base. It is singular to reflect that these 
 deposits, which, if they were located in England, would be colossal fortunes for their 
 owners, are at present absolutely valueless owing to their geographical position. 
 
 * General Report upon the Northern District. Brisbane: by Authority : 1870. 
 
ect; 
 
 ‘ 
 £ 
 & 
 
 
 
 23 
 
 CHARTERS TOWERS AND CAPE GOLD FIELDS. 
 
 These goldfields, although both geographically and geologically distinct, are 
 generally grouped together. They have for the greater part of their existence been in 
 the charge of the same Warden, and the returns from each have not always been kept 
 separate. The Cape, although at one time a rich alluvial field, has of late years 
 
 ‘diminished in relative importance, so that at the present day its output does not 
 
 seriously affect the total yield of the two fields, 
 
 In Daintree’s Report on the Cape River Diggings, &c.,* it is said that payable 
 gold deposits were “confined to the south-eastern outcrops of a vast thickness of schistose 
 rocks developed on the ‘Cape’; the north-western extension of the same having failed to 
 yield the precious metal in remunerative quantities to the prospector.’ The metamor- 
 phic schists are divided by him into Upper, Middle, and Lower. The Upper is composed 
 of hard quartzites and silicified mica slates. The Middle consists of soft thin-bedded 
 mica slates, with occasional bands of silicified mica and hornblende schists. In the Lower 
 subdivision, laminated granite, and mica- and hornblende-slates are interstratified ; and it 
 is in this portion of the series that transmutation of the schistose rocks is most marked. 
 Indeed, near the junction of the schistose and granite rocks, so great has been the 
 alteration that it is difficult to say where the schists end and the granite commences. 
 
 “No fossils have yet been, or are likely to be, met with in these beds on account 
 of their metamorphic character throughout. The only assertion to be made in regard 
 to their age is, that rocks of a similar character further north are unconformably 
 overlaid by others containing abundance of Upper Silurian fossils.” + 
 
 In the map attached to the Report the metamorphic rocks are provisionally 
 classed as “ Lower Silurian.’ The Report further mentions that where elvan or 
 porphyritic dykes traverse the metamorphic rocks the richest gold deposits were always 
 found. In some cases there was reason to suspect that “the rich quartz veins were a 
 continuation to the surface of the elvan veins themselves.” 
 
 Mr. Rands, in a recent Report,{ to which the reader is referred for a description 
 of the various reefs and leads, refers to these schists as follows :— 
 
 “The Cape River Gold Field comprises a series of schists and quartzites of vast 
 thickness, extending for a distance of over 50 miles in length, with an average of about 10 
 miles in width. The schists ‘strike’ about W.N.W. and E.S.E., and have an average 
 dip of from 30° to 35° to the S.8S.W. As there is no sign of folding or repetition of 
 the rocks, the same dip continuing throughout, this would give a thickness of between 
 5% to 6 miles of these rocks; nor is this even their entire original thickness, for to the 
 north-north-east their place has been taken by intrusive granite, leaving only here and 
 there traces of the original schists. 
 
 “ The schists in reality extend to a much greater distance in the direction of their 
 ‘strike,’ but they are covered with basalt. Jor instance, just north of Lolworth there 
 are two small hills, ‘inliers’ of schist, and the same rock crops out at Cargoon Station. 
 The schists of the Woolgar Gold Field are probably a continuation of the same series, 
 separated by a large layer of basalt, and they are probably continuous with the schists 
 of the Gilbert River, separated only by beds of overlying ‘ Desert Sandstone.’ How 
 far in the opposite direction—to the east-south-east—they extend it is impossible to say, 
 as the country is all a large alluvial flat. 
 
 
 
 
 
 * Brisbane: by Authority : 1868. 
 + Mr. Daintree probably referred to the Broken River, where rocks of a similar character are 
 
 overlaid unconformably by a limestone charged with fossils. The fossils, however, turned out to be 
 Devonian. 
 
 t On the Cape River Gold Field. Brisbane: by Authority : 1891. 
 
24 
 
 “ The lower portion of this series of schists—that which extends along the north- 
 north-eastern part of the field, and includes Mount Davenport and the Upper and 
 Lower Cape—consists of mica and hornblende schists into which granite has intruded 
 to such an extent that the area occupied by the granite is greater than that of the 
 original schists. There is also an interbedded and somewhat laminated granite in this 
 portion of the field, which may be due to extreme alteration of the schists. 
 
 “ Above this is a great thickness of mica schists with thin beds of hornblende 
 schists; these rocks are softer, and have been worn away to a great extent by dennda- 
 tion, leaving large alluvial flats, with here and there small rounded hills of somewhat 
 harder schist, which stand out prominently. 
 
 “The highest portion of the series—that extending along the south-south- 
 western portion of the field—consists chiefly of quartzite with hardened schists, which, 
 on account of their hardness, have resisted denudation, and have determined the rough 
 and hilly nature of this part of the field. The long spur, running in an east-south- 
 easterly direction from the main dividing range at Mount Miller to Mount Remarkable, 
 a distance of about 30 miles, is composed almost entirely of quartzite. 
 
 “Mr. Daintree, on lithological grounds, divided these beds into three divisions— 
 the Upper, Middle, and Lower. In the absence, however, of any fossil contents—and 
 they are not likely to be met with in rocks so much metamorphosed—and as the deposi- 
 tion of the strata appears to have been continuous throughout, I do not think there is 
 sufficient reason for keeping up these divisions. 
 
 “With reference to the age of the schists, I can say nothing more than that they 
 are the oldest rocks of the district, as the granite to the north-north-east does not form 
 the base or bed on which they were originally deposited, as intimated by Daintree, but 
 has since intruded into the schists.” 
 
 Free gold is found in the alluvia of the present watercourses, generally in the 
 vicinity of rich quartz reefs. But an older fragmentary drift, which Mr. Daintree calls 
 Pliocene, yields gold of a rounded waterworn character, independent of any local source 
 of supply. Several well-defined leads are mentioned, which, “down the Cape so far 
 as the Lower Diggings,’’ and down Running Creek as far as the junction of Golden 
 Gully, may be considered as the representative of old river channels; beyond these 
 points, to the south and east, it can be regarded in no other light than that of accumu- 
 lated sediment from a vast lake or sea. It has been found in working that where this 
 supposed old watercourse is narrowest the gold is most concentrated; but when it 
 becomes broader and the drift deeper, the gold is found to be too scattered to pay for 
 the additional cost of mining. 
 
 Of these Lower Cape Diggings, Mr. Rands (Joe. cit. p. 6) gives the following 
 further particulars :— 
 
 “The Lower Cape, or Capeville as it was formerly called, is situated on the Cape 
 River, about 3 miles above Hawthorn Vale Station. Nearly all the workings at the 
 Lower Cape are on what is known as the ‘Deep Lead.’ This was worked first about 
 eighteen years ago, and attracted a population of over 3,000; now the population is not 
 over 30, including the Chinamen. 
 
 “The lead has been worked in a southerly direction from the river for 25 miles. 
 The lead is both narrow and shallow; near the river it becomes deeper, and widens out 
 towards the south. Near the surface the drift consists of a decomposed schistose 
 material with pebbles of quartzite, granite, and quartz throughout it. The wash, in 
 which the gold occurred, consists of large rounded pebbles of a glassy-looking white 
 quartz, cemented loosely together by a schistose débris. The wash, as a rule, was from 
 i foot to 18 inches, aud in places as much as 2 feet, in thickness. The gold was 
 
25 
 
 coarse, and very much waterworn and. rounded, of a very different character to the mote 
 or less angular particles obtained from the gullies. The washdirt went from 1 oz. 
 to as high as 25 oz. of gold to the load, averaging nearly 3 oz. to the load. 
 
 “The most northerly point at which this lead has been worked is about 300 
 yards south of the river, and about the same distance west of the township. The depth 
 of the drift here was 38 feet; and then it became shallower opposite the township, 
 being only 15 feet deep. Just north of Gahn’s Flat the surface is being worked by a 
 sluicing company. The water for sluicing is pumped up from the river flat into tanks 
 by asmall engine. The quantity of water was quite insufficient for sluicing on a large 
 enough scale to make it pay. The returns have been very poor, with the exception of a 
 few patches of small nuggets which were met with. The drift spreads out over Gahn’s 
 Flat and then crosses a low ridge known as Red Hill. The depth here was only about 
 3 feet, and the whole of it was worked, yielding about 3 oz. of gold to the load. The 
 drift on this hill is coloured red with oxide of iron. Towards the south of Red Hill 
 it becomes deeper, and is about 15 feet deep. Immediately south of Red Hill is White 
 Hill, where the drift changes quite suddenly to a white colour. From this point it 
 gradually gets thicker, until at a distance of 2} miles the shafts are from 90 to 
 100 feet in depth, and the lead has spread out from a couple of hundred yards to 
 half-a-mile across, the gold here being more disseminated, going only about }-oz. 
 to the load, and the greater depth to which the shafts had to be sunk to bottom 
 caused the lead to be abandoned. Very little prospecting has been done south of 
 this point to ascertain whether a channel exists in which the gold would be more 
 concentrated. 
 
 “The late prospecting party which was receiving Government aid simply put 
 down a few holes in close proximity to the old workings at both ends of the lead. To 
 thoroughly prospect it a series of holes, connected with drives, should be put right 
 across the drift some distance in advance of the last working places. 
 
 ‘“¢ A few holes were put down near Murray Creek, 3} miles south of the township, 
 but without any results. 
 
 ‘‘ In wet seasons, when there is plenty of water about, men make a living fossick- 
 ing over the old workings. It might pay to sluice the whole ground over if the difficulty 
 of obtaining water could be overcome. 
 
 “ Large quartz reefs occur in the schists on both sides of the lead. They are 
 composed of a hard, glassy, barren-looking quartz. 
 
 “ On the northern side of the river, between a point opposite Charters Creek and 
 Sandy Creek, known as Milkman’s Point, very rich gold has been obtained in a drift 
 similar to the above, with the exception that granite boulders are more numerous. The 
 drift on this flat is between 40 and 50 feet deep. A large portion of this ground is 
 still unworked on account of the great amount of water met with. Between Rocky 
 and Sandy Creek the wash went 6 oz. of gold to the load. A good deal of surfacing 
 has been done here too. 
 
 “ A deep drift was worked on the south side of Sandy Creek, opposite China- 
 man’s Gully, about 33 to 4. miles up above its junction with the river. 
 
 “ As to the age of these drifts it is impossible to say more than that they are 
 considerably older than the alluvial deposits of the present watercourses. It is very 
 probably a Tertiary deposit. It is impossible without a detail survey to define its extent 
 south of Bett’s Creek, but much of the country coloured Pliocene Tertiary on Daintree’s 
 map is recent alluvium. 
 
 “ Chinaman’s Gully was exceedingly rich throughout its whole length. The bed 
 of the gully is very narrow, and the gold was therefore concentrated in a small space. 
 
26 
 
 The gold was coarse and nuggetty. A large flat nugget of 90 oz. was found by the 
 Chinamen, as well as several others ranging in weight from 2 to 20 oz. The gully was 
 discovered by Chinamen, and has been worked over three successive times by them. 
 The gold is somewhat similar to that got in a drift near the head of the gully, and may 
 have come from there. At the time of my visit two miners were sluicing the surface on 
 the west side of the gully. The water was conducted through a water-race 3 miles 
 in length, from a creek at the foot of the granite range. 
 
 ‘“‘Payable gold has been got in most of the gullies around Mount Elvan. Three 
 leads have been worked at the Upper Cape. 
 
 “The Canton Lead is situated on the western side of Gorge Creek. It runs 
 in a direction W. 35° S. from a small gully called Little Bargoo Gully. The gold 
 got in this gully was of the same character as that in the lead. At the mouth of this 
 gully the same hypersthene-rock dyke crops out that is met with on Daunton’s Hill. 
 Payable gold was taken from surface workings at the head of the lead The breadth 
 of the lead near its head is about 30 feet, and its depth about 15 feet. The country on 
 both sides of it is schist. Further down, where it junctions with a branch lead from 
 Surface Hill, it is 100 feet in breadth. 
 
 “The drift consists of flat pebbles of schist, and rounded pebbles and boulders 
 of granite. It has a horizontal stratification. The wash at the bottom consists of 
 much coarser pebbles. The gold was chiefly wire-shaped. 
 
 “It has been worked entirely by Chinamen; they were sluicing it away in a face 
 of about 25 feet in depth at the time I was there, The branch lead, heading from 
 Surface Hill on the eastern side of Gorge Creek, was being sluiced by Daunton and 
 party in Daunton’s Gully. It is only in rainy seasons such as that of last year that 
 water can be procured for sluicing purposes. . 
 
 “The Pot-hole Lead is situated a little over a mile below the Upper Cape, on 
 the south side of the river. In the river at the mouth of the lead there is an intrusive 
 felspar porphyry of a reddish chocolate colour, which, in thin sections under the micro- 
 scope, shows an undistinguishable groundmass having a flowing structure, full of ferrite 
 and magnetite, and containing porphyritic cry stals of ligoclaae felspar. This rock 
 extends for over half-a-mile down the river. 
 
 ‘Close to the river the drift is only 12 feet in thickness. The wash contains 
 large boulders of granite, some of them over 2 feet in diameter. Pebbles of red oxide of 
 iron occur in the drift, and are looked upon as a good indication of the presence of gold. 
 Two hundred yards ti of the river the average depth of the shafts is 30 feet. A few 
 pebbles of olivine basalt oecur here, and also small pieces of rounded olivine, called 
 ‘green painters’ by the miners, which are said to be a certain indication of gold in the 
 wash. The presence of the basalt points to the fact that the drift must be of a great 
 age, as no basalt occurs in the district now, with the exception of the dyke before 
 mentioned, and that on Mount Black, about 6 miles up the river from here. The basalt 
 pebbles are probably the detritus of the basaltic outflow of which the small patch on 
 Mount Black is now the only remnant. ‘he other materials of the drift are similar to 
 those in the Canton Lead. 
 
 “The Bluff Lead was being worked by Chinamen about a quarter of a mile north 
 of the above. It is of the same character as the drift deposits.” 
 
 In 1867 the Warden estimated the population of the Cape at 900 Europeans and 
 100 Chinese, but gave no estimate of the gold produced. Before the Department of 
 Mines began (in 1877) to publish Annual Reports, the population and production had 
 greatly declined. In 1878 the population was estimated at 50 Europeans and 45 
 Chinese, and the production of gold at 3,000 oz.; in 1879 the estimated yield was 
 
oe «Fe @ 
 
 27 
 
 2,400 oz.; in 1880,* reef gold 442 oz., alluvial 615 0z.; in 1881,* estimated total 
 3,000 oz.; in 1882,* estimated total 3,000 oz.; in 1883,* reef gold 200 oz., alluvial 
 1,000 oz.; in 1884,* estimated total 1,944 oz.; in 1885,* estimated total 1,000 oz.; in 
 1886,* estimated total 500 oz. ; in 1887,* reef gold 987 oz., alluvial 124 oz.; in 1888,* 
 estimated total 328 oz.; in 1889,* reef gold 643 oz., alluvial 1,058 oz.; and in 1890, 
 estimated total 2,020 oz, 
 
 The Charters Towers Field stands first among Australian gold-producing areas. 
 It will be seen that the above returns from the Cape are so small as scarcely to affect 
 the totals credited to Charters Towers. 
 
 The richest part of the goldfield lies on the western edge of a large area of 
 granitic rock. The granite varies from a type in which orthoclase felspar, mica, and 
 quartz are the essential minerals, and hornblende an occasional or accidental mineral, to 
 a type in which, in addition to the constant orthoclase and quartz, hornblende is the 
 essential and mica the occasional mineral. Reference may be made to Mr. A. W. 
 Clarke’s Micro-Petrographical Notes. (See post.) 
 
 West of the granite several reefs are worked in less highly metamorphosed rocks, 
 but not only are these reefs less rich in gold, but the gold is also more alloyed with silver. 
 These rocks consist of quartzites, greywackes (of mixed quartz, felspar, and hornblende 
 granules, with some mica), shales, and slates. The slates and shales are highly impreg- 
 nated with iron peroxide. The stratified rocks strike as a rule N.W. and S.E., and 
 dip at over 45° to N.E. and 8.W. They afford no direct evidence of their age, but are 
 covered unconformably by the Middle Devonian Limestone of Burdekin Downs. 
 
 The reefs in the central portion of the field have no uniform trend, but they 
 have invariably an underlie to the north side of their outcrop, and generally at a 
 comparatively low angle. 
 
 Down to the water-level the gold was “free” in a gangue of granitie débris and 
 quartz, mixed with “brownstone” or decomposed pyrites. Below that ievel the gold 
 occurs in quartz associated with a “ mundic” composed of pyrites, galena, and zinc- 
 blende, which has not proved hard to treat. 
 
 The greatest depth at which gold has yet been worked is 1,500 feet (vertical). 
 This is in the Mills United Mine. 
 
 About sixteen miles south of Charters Towers gold occurs in thready hematite 
 veins, which reticulate through a volcanic “ Neck,” acta dl Mount Leyshon. This neck 
 has been pierced partly through greywackes and slates, and partly through a porphyry. 
 The porphyry is composed of straw-coloured silicated felspar, with crystals of orthoclase 
 felspar and quartz, the latter occurring, however, most frequently in rounded blebs. It 
 sends out veins through the greywackes and slates, and also through the granite which 
 occurs to the north. The Neck is the once deep-seated pipe or core of a volcano, 
 filled up with the fragmental material which supplied the ashy outbursts. This 
 material varies considerably in texture, some portions being merely aggregations of fine 
 felspathie dust, while others are agglomerates of coarse angular débris of broken 
 porphyry, cemented together by a sparse matrix of dust felted with iron oxide. 
 Broken crystals and rounded blebs of quartz are scattered throughout the matrix; in 
 fact, the material is exactly such as could be manufactured from the waste of the 
 porphyry. Crystals of felspar in some cases appear to have been developed in the ash, 
 so that but for the granular and clastic appearance of the matrix, the resemblance to 
 the adjacent porphyry rocks would be complete. The rock has for some time paid for 
 passing through the stamps as a whole, picking the auriferous veins being an 
 impossibility. Now and then larger masses of auriferous stone are met with. In the 
 
 
 
 
 
 * Rands, loc. cit., p. 18. + Warden’s Report for 1890. 
 
28 
 lower levels auriferous iron and copper pyrites begin to be met with, and it is possible 
 that deposits concentrated in reefs will be discovered. The Neck is of considerable 
 extent, covering nearly 200 acres, and is auriferous from its northern end to its south- 
 western extremity (Wallaby Point). It is singular that in the adjacent twin neck, 
 Mount Mawe, the existence of payable gold has not yet been proved. 
 
 The total yield of Charters Towers and the Cape up to 31st December, 1890, is 
 estimated at 2,078,531 oz. How much of this came from the Cape it is now impossible 
 to say. During late years the amount has been comparatively insignificant, but it is 
 probable that for the six or seven years prior to the opening of Charters Towers (in 
 1872) it was of considerable importance. 
 
 AVERAGE YIELD PER TON OF STONE CRUSHED AT CHARTERS TOWERS. 
 
 
 
 
 
 Oz. dwt. gr. Oz. dwt. gr. 
 
 1877 EP pelGr 22 1884 2 One 
 
 1878 110 is 1885 1 18 9 
 
 1879 1 10 Fis 1886 eel 7, 4 
 
 1880 1 ae ee 1887 ie its} 6 
 
 1881 1 10 12 1888 J) Sis 
 
 1882 1 14 419 1889 1 10 9 
 
 1883 ne ae lly¢ 1890 i 5 18 
 
 YreLD oF CHARTERS TowERS AND Cape Goup FIELps. 
 REEF GOLD. | 
 Year. Alluvial Gold. Total Gold. Remarks. 
 Tons of Quartz} Oz. of Gold 
 Crushed. therefrom. 
 To end of— Oz. Oz. : 
 1875 nor 442,976 1 | } Deduced from figures in Report 
 1876 - 39,463 Pee 67,616 of Department of Mines for 
 1877 21,929 2 36,030 66,479 88,408 1872, p. 10. 
 1878 18,849 2 35,510 53,340 72, IAS lla ns Ba: 
 1879 17,461 2 41,584: 63,568 3 81,029 | > “ Tailings and alluvial. 
 1880 16,704 ? 39,285 68,594 8 85,298 $ S : 
 1881 Re 45,378 82,324 5 82,324 een include <gold saris 
 1882 100 6 45,662 79,495 7 79,595 say 
 1883 1,000 ® 44,602 68,559 69,559 | « Not estimated. 
 1884 3,090 ° 52,568 106,236 109,335 
 1885 1,000 ° 70,164. 134,650 135,650 | ® Includes gold from pyrites. 
 1886 Oe o> 77,665 144,379 144,379 : 
 1887 317 6 83,292 151,060 151,377 | ° Alluvial only. 
 1888 5 rig 81,698 117,432 137,522 ; =e 
 1889 1,900 ® 108,828 165,352 167,252 7 Includes gold from tailings. 
 1890 8,786 7 121,406 155,236 164,022 | s «Tailings, alluvial, &c.” 
 Total 2,078,531 9 “Tailings, &c.” 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 GILBERT AND WOOLGAR GOLD FIELDS. 
 
 These fields, although coterminous with the Etheridge, differ from it essentially 
 in their geological characteristics. The divide between Caledonia Creek (one of the 
 heads of the Delaney River, a tributary of the Etheridge) and the Robertson River (a 
 tributary of the Gilbert) is dotted over with little fragmentary tablelands of Desert Sand- 
 stone. The latter formation, as mapped by the late Mr. Richard Daintree, occupies 
 considerable areas in the Newcastle and Gregory Ranges, and between Agate Creek and 
 the Perey River. The conglomerate beds of the formation are rich in agates, topazes, 
 garnets, and other precious stones, including, it is said, rubies, sapphires, and diamends.* 
 Another belt of the Desert Sandstone makes its appearance at the heads of the Woolgar, 
 
 
 
 Mr. Warden Samwell in Report of the Department of Mines for 1873. 
 
29 
 
 where it is capped by basaltic rocks, probably of Tertiary age. Beneath the Desert Sand- 
 stone lie the metamorphic auriferous rocks of the Gilbert and Etheridge Gold Fields. 
 
 According to a geological map of the Gilbert, published by Daintree in 1869, 
 the country near the junction of the Robertson with the Gilbert is composed of “ slates, 
 shales, &e.,” of Lower Silurian age, skirting west-north-west. Regarding the age of 
 the rocks in question, I am not aware that there is any direct evidence beyond their 
 general lithological resemblance to Victorian Lower Silurian rocks. The upper 
 waters of the Robertson and heads of the Gilbert are mapped as ‘“ metamorphic-mica 
 schists” striking west-south-west. These and the “slates, shales, &c.,” are penetrated 
 by numerous dykes of “elvanite, diorite, hornblende rocks, &.,” and it is noted that 
 “ where these elvanites penetrate slates, payable gold is usually obtained.” 
 
 The geological characteristics of the Woolgar Gold Field are similar to those of 
 the Gilbert. 
 
 The output of the Gilbert is impossible to estimate, as the returns have been 
 hopelessly mixed up with those of the Etheridge. In 1877 the Warden reported that 
 in the years 1869-1872 the field “ gave employment to a large number of European and 
 Chinese miners, but from a variety of reasons it has been entirely abandoned for 
 upwards of three years, but it is again showing signs of renewed activity.” 
 
 In 1878 there was a considerable accession to the population engaged in alluvial 
 working, and preparations were being made to re-open abandoned reefs. In 1879 the 
 earnings of 500 Chinese were estimated at a minimum of 7,000 oz. of gold. In the 
 same year the Gilberton Gold-mining Company crushed 420 tons of stone for a yield 
 of 142 oz. 15 dwt. In 1880 the alluvial diggings were estimated to have yielded 
 6,260 oz. Jn the Warden’s reports after 1880 no separate estimate is made. In 1885 
 the Warden reported that the Mount Hogan and Twenty-mile Reefs had crushed 
 during the year 162 tons for 365 oz. of gold. 
 
 In 1887, 450 tons of stone were crushed at Mount Hogan, for a yield of 1,030 oz. 
 of gold, and the population of Gilberton had dwindled to two Europeans. In 1888 the 
 Mount Hogan machine crushed 1,112 tons for 1,958 oz. For 1889 Iam unable to 
 give the yield of Mount Hogan, but the Gilberton machine is reported by the Warden 
 to have crushed 207 tons, the crushing giving over 1} oz. to theton. In 1890, a 10-head 
 . battery was fully employed at Mount Hogan during the whole of the year, and 1,159 
 oz. 19 dwt. 3 gr. of gold were sold to the Charters Towers banks. At Gilberton 
 little crushing had been done during the year, but the Charters Towers Warden reports 
 108 oz. 19 dwt. 18 gr. of Gilberton gold purchased by the banks. 
 
 In the case of the Woolgar, the returns up to 1882 are to some extent mixed up 
 with those of the Etheridge, but, so far as they can be separated, the following are taken 
 
 from the Warden’s books :— 
 YIELD oF WooLGAR GoLp FIELD. 
 
 
 
 
 
 
 
 
 
 
 
 Year. Tons of Stone Yield of Gold. Alluvial Gold. Total Gold. 
 Crushed. 
 Oz. Oz. Oz. 
 1880 ... AB or Sey 5 ae 2,500 2,500 
 1881 ... oe a ae — oe 500 500 
 1882* pe 4 ae eS: is ee 
 18838 ... is os sie 1,200 2,4.00 200 2,600 
 1884... 1,734 1,976 350 2,326 
 1885 ... 5,006 3,940 nae 3,940 
 1886 ... 2,819 2,079 350 2,429 
 1887 ... 694. 709 ne 709 
 11,453 11,104. 3,900 15,004 
 
 
 
 
 
 
 
 * Returns included in those of the Etheridge, 
 
30 
 
 In 1888 the Warden reported the field briefly as ‘‘ dormant,” in which condition 
 it may be said to remain, although the Charters Towers Warden mentions 461 oz. of 
 Woolgar gold purchased by the banks in 1890. 
 
 “Galena carrying silver is found in abundance on the [Gilbert] field. Near 
 Gilberton three parties of men are opening galena lodes, from which some good assays 
 of silver have been obtained. At the Perey River rich bismuth ore is found in gullies 
 formerly worked for alluvial gold. Three men worked this ground for some time, and 
 stacked a large quantity of washdirt containing ore. They also discovered a reef carrying 
 the ore in small quantities. The absence of a market for the ore in the colonies, and 
 the uncertainty as to the price obtainable in England, have had the effect of discouraging 
 the miners, and work has now been discontinued.”* The ore referred to is the car- 
 bonate of bismuth, and what samples I have seen of it are almost chemically pure. 
 “The principal lodes are found towards Gilberton, viz.—Galena, large, carrying a good 
 percentage of gold and silver, and pure galena; bismuth, and bismuth and copper; 
 copper ; silver, with lead and sulphur; silver; silver and antimony; and so on. They 
 are of various colours, and some of the lodes are of great width, and traced for miles 
 along the surface of the ground. Tin is also met with, tin and copper having been 
 worked on the east of the Hinasleigh River.’+ “Silver in galena lodes, with a 
 percentage of gold and indications of copper, exists on the Woolgar.’ 
 
 COEN GOLD FIELD. 
 Ags an alluvial field, the Coen had a short existence (from February to July, 1876). 
 The country-rock is granite, greywacke, mica-schist, and quartzite. The alluvial gold 
 was poor in quality and insufficient in quantity. Several reefs occur in the neighbour- 
 hood of the diggings. One of these, the Llankelly, has been worked profitably for a few 
 
 years back. 
 NORMANBY AND MARENGO GOLD FIELDS. 
 
 NoORMANBY. 
 
 There are no less than three goldfields in the Colony known as Normanby. The 
 one here referred to lies about forty miles south of Bowen, on the heads of the Dart 
 and Grant, tributaries of the Broken River. 
 
 The goldfield occupies a portion of the Clarke Range. That range consists 
 almost entirely of metamorphic rocks. That these have undergone metamorphism, 
 followed by extensive denudation, prior to the date of the Lower Bowen River forma- 
 tion, is proved by the relations they bear to the Bowen River Coal Field. In some places 
 shales, slates, quartzites, greywackes, lydian stone, and mica and hornblende schists are 
 met with; and there is little doubt that the whole tableland was originally composed of 
 stratified rocks. In the immediate neighbourhood of Normanby, however, the occur- 
 rence of stratified rocks is notably rare, and the country-rock mostly consists of a species 
 of porphyry, composed of quartz, black mica (sparsely), and crystals of schorl. The whole 
 rock is mixed up with minute crystals and streaks of pyrites, and streaks and veins of ser- 
 pentine. Occasional sections show a passage from greywacke to the rock just described. 
 
 In 1872-8, the Hibernia, Grace Darling, Marquis, Welcome, Star of Hope, 
 Albion, New Zealand, Venture, and other reefs were at work, and everything went well 
 till the water level was reached, crushings of from 1 oz. to 23 oz. being the usual 
 return. At the water level, however, “mundic” took the place of the easily reduced 
 “brownstone,” and as at the time the treatment of complex auriferous ores was little 
 understood, the claims one after another were abandoned, although the stone assayed 
 
 
 
 * Warden’s Report in Report of the Department of Mines for 1881. 
 + Mr. Warden Samwell’s Report in Report of the Department of Mines for 1883. 
 ~ Mr. Warden Samwell’s Report in Report of the Department of Mines for 1886, 
 
~~ 
 
 31 
 
 sometimes as much as 8}0z. to the ton. The field suffered for many years from an 
 unjustly acquired bad reputation ; had it been discovered fifteen years later it would 
 probably have entered at once on a course of unchecked prosperity. 
 In 1888 several of the abandoned reefs again set to work, and the yield is set 
 down as 205 0z. In 1889, 109 oz. are credited to the field. Both of these amounts 
 probably represent alluvial gold, as crushing machinery had been erected but not started 
 to work. In 1890, 759 tons of stone yielded 569 oz. of gold, 189 oz. of alluvial gold 
 bringing the total to 758 oz. Recently some of the mines are reported to be on rich stone. 
 From 1877 to 1883 the Annual Reports of the Department of Mines give the 
 following statistics of gold from “ Normanby, Marengo, and Mount Wyatt.” The 
 
 greater part must have come from Normanby, and was probably chiefly alluvial gold :— 
 Oz. 
 
 57 Ee ee A ck ein Fe ee © 820 
 2 SCE co, ee en ge I ate ae ey GSS 
 a ee cee ee | ee Pe Pio 
 Doc Tt. Se AY Bk eT SEAS 
 Ton ee er Wee AE) tol SADIE oie ng cule Oy BiB 
 hse head oes Pasa hl 8 8 Ue Oo, | B08 
 St meats Cm ee PW hee pat Wo kien yi 201 
 
 E Tome. cure ee Slee ae!) SA 2°788 
 
 MARENGO. 
 
 This smali field lies about twenty-three miles south-west of Bowen, on a low 
 tableland dividing the head waters of the Bogie from the parallel valley of the Don. 
 The lithological description of this limited area may be applied to the whole of the range 
 between the Burdekin and the coast—essentially a white granite, in which the mica is 
 sometimes supplemented and occasionally replaced by hornblende, frequent bosses of 
 intrusive pale pinkish felspar-porphyry (the felspar highly acidic), and occasional small 
 areas of gneiss and mica-schist and of little metamorphosed, or at least still recognisable, 
 shales and greywackes. The description of the field ought properly to have been placed 
 in the preceding Chapter, but is more conveniently included here, on account of its 
 geographical connection with the Normanby Field. 
 
 About a dozen reefs were worked for a short time from 1871, but proved too 
 
 
 
 ‘poor for profitable working at the time, the crushings varying from 3 dwt. to a little 
 
 over 1 oz. per ton. The caps of the reefs showed a good deal of carbonate of copper, 
 and the gold was soon found to be mixed with copper and iron pyrites. With 
 economical working, Marengo and numerous other fields similarly situated will some 
 day pay to work. One or two of the reefs are good enough to pay now, but could not 
 bear by themselves the whole of the expenses necessary to put the field in going order. 
 A goldfield in its infancy offers an exception to the usual laws of trade. The mines 
 must bear in common the expenses of the machinery, &¢., without which they are 
 themselves worthless. Instead, therefore, of there being a struggle for existence, each 
 individual miner is directly interested in his neighbour’s prosperity. 
 
 PEAK DOWNS GOLD FIELD. 
 
 The reefs in this goldfield occur in an area of crumpled and fissured metamorphic 
 schists, slates, &c., near the township of Clermont. Daintree, in his “ Geology of 
 Queensland’’* refers these rocks to the ‘“ Lower Silurian Series, or even to the still 
 older metamorphic system of Victoria,” but the only direct evidence of their age is 
 that a bed of limestone, apparently of Devonian age (Burdekin Beds), appears to lie 
 unconformably on them. “The principal reefing country lies to the south of Clermont, 
 
 
 
 
 
 * Quart. Journ, Geol, Soe., vol. xxvili., p. 301, 
 
32 
 
 and extends from 2 to 3 miles west of Copperfield to Macdonald’s Flat, a distance of 
 about 7 miles. The reefs have a general east-and-west trend. In none of them can 
 the work be said to have gone beyond the prospecting stage. I must point out that 
 the depth to which these reefs have been tried exceeds in no ease 150 feet or 160 feet, 
 and only in a few eases has this depth been reached. The returns of the crushings, 
 too, that have been kept do not give a fair account of their average yield of gold, for 
 the returns of the earlier and best crushings have been Jost. I certainly am of opinion 
 that some of them will be found payable at deeper levels.” (Rands.) 
 
 “Most, or I might say practically all, of the gold sent away from this field has 
 been the yield of alluvial workings. Ever since the year 1862, when the first rush took 
 place, thousands of ounces of alluvial gold have yearly been obtained. The returns of 
 the gold sent away in earlier years have not been preserved. The yield, however, was 
 much larger than of late years. This falling-off has been caused, to a great extent, by 
 the dearth of water.” (Rands.) 
 
 In addition to diggings in the recent alluvia of the gullies on both sides of the 
 Drummond Range, gold has been obtained in large quantities from drifts covered by a 
 flow of basalt. The Victoria Lead has been, perhaps, the richest deposit of gold in the 
 district. At the summit of the hill, where the workings on it started, the washdirt was 
 only 15 or 20 feet deep. About three-quarters of a mile to the north, where it ran 
 under the basalt, it was 100 feet deep. Its average width is from 20 to 30 feet. A 
 30-0z. nugget was obtained from near the head of the lead. The washdirt is said to 
 have averaged 13 oz. to the load all the way through, and 24 loads in one part went 8 oz. 
 per load. Daintree, in his “Geology of Queensland,” says, with reference to the 
 voleanic outbursts: “The more northern volcanic areas, those shown on the map north 
 of lat. 21°, are probably contemporaneous with the upper volcanic series of the Victorian 
 Geologist, and are probably of Pliocene-Tertiary age. Tbe southern areas, viz., Peak and 
 Darling Downs, &c., are older, agreeing with the Lower Volcanic of Victoria, which have 
 been ejected through fissures, and have in no casea very extensive flow beyond the line of 
 fracture through which they have issued. These may be referred to the Miocene epoch.” 
 
 A still older, and in some respects a very remarkable, auriferous drift oecurs in 
 the Cement Hill, at Hurley’s, and at the Four-mile. Cement Hill is described as con- 
 sisting of ‘ Firstly, from 15 to 80 feet of a conglomerate composed of boulders and 
 pebbles of schist and small quartz pebbles, the whole cemented together by a clayey 
 cement formed by the disintegration of the schist itself. This conglomerate is soft, 
 but very tough to work in. The bottom 4 or 5 feet forms the washdirt in which the 
 gold is found. Secondly, underlying the conglomerate is a fine-grained silt or shale 
 from 1 to 4 feet in thickness, termed by the miners ‘dig,’ which is cut away to facilitate 
 the bringing down of the wash above. Lastly, another drift of smaller pebbles and not 
 auriferous. This rests on the auriferous schists of the district. The ‘dig’ contains 
 Glossopteris, the characteristic plant of the Bowen River and Newcastle (N.S.W.) 
 Beds, and therefore the deposit appears to belong to Carbonifero-Permian Series. The 
 auriferous portion of the upper conglomerate or drift is said to contain, as an average, 
 about 5 or 6 dwt. of gold per ton.’’* 
 
 The above conclusion was quite warrantable while the presence of Glossopteris 
 was understood to be an infallible test of the Paleozoic age of the strata in which it 
 occurred. Such reasoning, however, has now entirely lost its force since Mr. Rands’ 
 discovery of Glossopteris in the Desert Sandstone.t 
 
 
 
 
 
 : * W. H. Rands’ Report on the Geology and Mineral Deposits of the Country in the Vicinity of 
 Clermont. Brisbane: by Authority: 1886. 
 
 + See remarks under ‘‘ The Organic Remains of the Desert Sandstone.” 
 

 
 33 
 
 The returns from the Peak Downs Gold Field are very imperfect. For the first 
 fifteen years of the history of the field I can only find one record by the Warden (of 
 4,900 oz., escorted in 1867). It cannot possibly be over the mark to fill up the blanks 
 in the record as I have done by taking 4,000 oz. as the average annual yield from 1862 
 to 1856 inclusive, and 3,000 oz. annually from 1868 to 1876 inclusive. The recorded 
 returns, with these additions, give a total yield of 110,853 oz. of gold. Gold to the 
 amount of 6,294 oz. is returned as the yield of 12,461 tons of quartz crushed, but it 
 must be remembered that Mr. Rands points out that the records of the earlier and 
 richer crushings have been lost. 
 
 YIELD OF Peak Downs Goup FIELD. 
 
 
 
 
 
 
 
 REEF GOLD, 
 Year. Alluvial Gold, Total Gold. Remarks, 
 Stone Gold 
 Crushed. therefrom. 
 Tons. Oz. Oz. Oz. 
 1862-1866 aa Aes nee 20,000! 1Hstimated. 
 1867 ae Fi Pe 4,9002 2 Escorted. 
 1868-1876 ace ann ave 27,0002 
 
 1877 Sih ate BAC 3,000 
 1878 2,6733 1,670 2,330 ? 4,000 3From Macdonald’s Flat reefs 
 1879 963 528 5,480 P 6,000 alone. 
 1880 2,293 1,089 6,311? 7,400 
 1881 2,545 758 6,718 7,476 
 1882 1,211 842 5,158 6,000 
 1883 484 243 OM Asie 3,000 
 1884 652 275 2,993 3,268 
 1885 213 119 3,545 3,664 
 1886 746 253 4,104 4,357 
 1887 486 310 4,108 4,418 
 1888 124 68 2.277 2,345 
 1889 71 139 1,947 2,086 
 1890 rit Sis 1,939 1,939 
 
 Total ... |. ae 110,853 
 
 
 
 
 
 PEAK DOWNS COPPER FIELD. 
 
 “This lode was discovered in 1862. It can be traced for over 1$ miles, running 
 in an east-and-west direction, It has an underlie varying from 40° to 70° to the 
 south. The country consists of foliated and contorted micaceous and hornblendic 
 schists, dipping south-east. The outcrop is a gossan, consisting chiefly of red and brown 
 hematite, with a little oxide of manganese, and carbonates of copper. The ores were 
 oxides and carbonates of copper to a depth of about 75 feet vertical from the surface, a 
 mixture of oxidised ores and sulphurets to a depth of 120 feet, and below that depth 
 they were ordinary sulphurets of copper. 
 
 “The gossan at the surface was auriferous; assays of it give from 4 dwt. to 
 1 oz. 16 dwt. of gold per ton, and also up to as high as 5 oz. of silver per ton. 
 
 “The deepest workings were 66 fathoms. Most of the lode was taken out to a 
 depth of 40 fathoms for a distance of half-a-mile. From 1862 to 1878, when the original 
 company was wound up, about 100,000 tons of ore, averaging 17 per cent. of copper, were 
 smelted at the company’s own works. That would give 17,000 tons of copper, the value 
 of which was over £1,250,000. Copper lodes, known as the ‘ Western Peak Downs 
 Copper Lodes,’ exist about 7 miles west of Copperfield. Rich sulphurets of copper 
 were obtained from these.” (Rands’ “ Geology, &c., of Clermont.’’) 7 
 
 G 
 
 . . 
 
CHAPTER IV. 
 
 MIDDLE DEVONIAN (BURDEKIN FORMATION). 
 
 ARGENTINE SILVER FIELD. 
 
 Rocks of Devonian age occur in at least five localities in Queensland—viz., the 
 Burdekin Valley, including the Broken and Fanning Rivers, the mountains north of the 
 Reid River crossed by the Northern Railway, Clermont Central Railway, and Hunter 
 and Marble Islands in the Northumberland Group. 
 
 It is possible and even probable that considerable areas coloured as schists, 
 slates, &c., of undetermined age may yet be recognised as belonging to the Devonian, 
 but for the present the localities above named are the only ones in which the presence 
 of Devonian rocks has been determined upon sufficient evidence. The Rev. W. B. 
 Clarke attributed a Silurian age to the slates, quartzites, &c., which cross the border of 
 New South Wales into Queensland at the heads of the Severn River. 
 
 Aplin, in his “ Report on the Upper Condamine,’* speaks of the Silurian rocks 
 extending connectedly along the southern border, but remarks on the fossils that “in 
 general aspect they resemble the fossils of the diorite slates at Gympie” (page 5). He 
 mentions only Productus and Spirifer, as occurring at Elbow Creek, Lucky Valley, 
 together with crinoids and corals. To his statement regarding the resemblance of the 
 fossils to those of Gympie, I attach greater weight than to his determination of two 
 genera of Brachiopods which range up to a much later date than Silurian. Daintree 
 (1872) appears to have regarded the greater part of the stratified rocks occurring in 
 the eastern ranges of the Colony, with the exception of the Coal Measures, as Devonian+; 
 and Mr. R. Etheridge, F.R.S., in his Appendix to Daintree’s Paper, massed the fossils 
 from the Gympie Beds with those from the Burdekin Beds as Devonian {—a classi- 
 fication which later collections have shown to be untenable. 
 
 Gregory, in his ‘‘ Geological Map of Moreton and Darling Downs (1879),”’ coloured 
 the altered slates and sandstones extending from near the border northward to near 
 Brisbane, and again from Brisbane to the heads of the Caboolture, as Devonian, and in 
 his Report on the Geological Features of the South-eastern Districts of the Colony § 
 describes them as such, and refers to the Gympie Beds as of the same age. 
 
 In my Geological Map, prepared for the Colonial and Indian Exhibition of 1886, 
 IT coloured the strata in the neighbourhood of Gympie as Lower Carboniferous, but had 
 not yet seen any reason for disagreeing with Daintree’s conclusions as to the Devonian 
 age of the remainder of the altered stratified rocks which extend, with some interrup- 
 tions, from Keppel Bay to the southern border. In my “ Handbook of Queensland 
 Geology” (Brisbane, 1886), I said (p. 28):— It is with considerable hesitation that I 
 class, in the meantime, the greater part of the Palzozoie rocks south of Marlborough 
 as belonging to the Burdekin Beds. It is quite likely that among the highly inclined 
 and much distributed rocks of this region strata will yet be found separable, on account 
 of their fossil contents and their stratigraphical relations, from the rest, and of 
 different ages. But fossiliferous limestones, apparently identical with the Burdekin 
 
 
 
 * Brisbane: by Authority : 1869. +t Loc. cit., p. 320. 
 + Quart. Journ. Geol. Soc., vol, xxviii, p. 288. § Brisbane: by Authority : 1879, p. 7. 
 
B5 
 
 Beds, are so common in the whole region, that the attempt to separate them from the 
 other strata, which, after all, present only the negative evidence of the absence of 
 fossils, has proved hitherto a task beyond our powers. Attempts have been made in 
 limited areas ; but I do not think that sufficient evidence has as yet been accumulated 
 to warrant the conclusions which have been drawn.” In another place (p. 37) 
 I added :—“ Some slates containing Fenestella, &c., from the Training Wall Quarries, 
 Rockhampton, forwarded by Mr. James Smith, so much resemble some of the Gympie 
 Beds that, in the meantime, I map a small area as of the same age.’’ Since then, 
 however, Mr. Smith (now deceased) has brought to light a considerable collection of 
 fossils from localities extending over the greater part of the Port Curtis District, as well 
 as from Kooingal, sufficient to prove the identity of the strata over this wide tract with 
 those of Gympie. Mr. Rands’ collections from Raglan, Langmorn, Calliope, the Boyne, 
 Cania, and Yarrol point to the same conclusion as regards these localities. The whole 
 of the district, therefore, from Lat. 22° to Lat. 26°, with the exception of some limited 
 areas of newer formations, has been removed from the Devonian and classed with the 
 Gympie Beds. 
 
 At Burdekin Downs, and for six miles up the Burdekin River, the outcrop of a 
 great mass of limestone is seen at intervals. The area occupied by its outcrop is marked 
 by a greener vegetation than that which covers the surrounding country. The limestone 
 must have formed a coral reef of great thickness. On its weathered surfaces the corals 
 stand out in admirable relief, like triumphs of the sculptor’s art. When the corals are 
 examined under the microscope their cells are seen to be filled with cale-spar. 
 
 At the mouth of a little creek falling into the Burdekin between Arthur’s Creek 
 and Burdekin Downs Station, the limestone dips at about 10° to the north-west and 
 rests directly on the granite. Its outcrop occupies half-a-mile, and its thickness should 
 therefore be about 450 feet. It is succeeded by a bed of fine-grained, white, hardened 
 sandstone or quartzite. 
 
 Arthur’s Creek is understood in the district to be the same as “ Terrible Creek, 
 near Messrs. Cunningham’s Cattle Station, Burdekin River,” described by the late 
 Mr. R. Daintree.* 
 
 The limestone is probably the same as that referred to by Leichhardt in his 
 “ Journal of an Overland Expedition from Moreton Bay to Port Essington during the 
 years 1844-5” (p. 241), in the following terms :— 
 
 “The opposite bank exhibited a very perfect and instructive geological section 
 of yariously bent and lifted strata of limestone, which were afterwards found to 
 contain innumerable fossils, particularly corals, and a few bivalve shells.” To one 
 coral in Dr. Leichhardt’s Collection, the late Rev. W. B. Clarke gave the name of 
 Cyathophyllum Leichhardt. 
 
 On the Fanning River, north of the Fanning Station, a bed. of limestone is seen 
 composed to a large extent of the remains of Corals, with a few Brachiopods and at 
 least one Cephalopod. Jn the above locality the limestone dips south-south-east at 20°. 
 Beneath the limestone beds are some beds of granitic sandstone with calcareous 
 concretions, the sandstone containing numerous impressions of Gasteropods, but the 
 matrix is too friable for removal. North of the station paddock the base of the lime- 
 stone ig seen very near a mass of granite, on which probably the beds beneath the 
 limestone rest. 
 
 East of the Fanning River the outcrop of the limestone forms a semicircular 
 band of low scrubby hills (on which the Bottle-tree appears to have a favourite 
 habitat), and returns to the river at the Old Station, five miles below the present station. 
 
 * Quart, Journ. Geol, Soc., vol. xxviii,, p. 290, 
 
36 
 
 Here the dip is to the west at 25°, and as the outcrop occupies a belt of four miles m 
 breadth, the total thickness of the limestone beds must be nearly 7,000 feet. From 
 the limestone near the Old Station I obtained, besides Corals, a few specimens of 
 Brachiopoda. A calcareous shale immediately above the limestone yielded, in addition 
 to corals and mollusca, the only plant—Dicranophyllum australicum, Dawson—yet 
 found in the Devonian rocks of Queensland. 
 
 The ring of limestone underlies a basin of stratified deposits, consisting for the 
 most part of grey, brown, and greenish flaggy sandstones, and greenish and chocolate- 
 coloured shales. A few of the sandstone beds are white, and would be well suited for 
 building purposes. From one of these white beds I obtained the specimen of 
 Dieranophyllum australicum which was described by Sir J. Wilham Dawson. 
 
 In the limestone of the scrubby hills above referred to are several large caverns, 
 beautifully festooned with stalactites and stalagmites. 
 
 The Broken River falls into the Clarke River, one of the most important 
 tributaries of the Burdekin, in Lat. 19° 80’ S. and Long. 145° E. Mr. Daintree, in 
 his Paper on the “ Geology of Queensland,”* wrote :—‘ On the track from the Broken 
 River to the Gilbert Diggings, Devonian rocks, several thousand feet thick, may be 
 observed, as they are continuous in dip, without being repeated, for at least five miles 
 
 across the strike, with an average inclination of 60° . . . . Onthe Broken River 
 and its tributaries a breadth of thirty miles, with a length of sixty miles, is occupied by 
 a persistent outcrop of Devonian strata. . . . . There the entire Devonian system, 
 
 as developed in Queensland, could be easily and satisfactorily mapped. The branches of 
 this river cut right across the strike, and the bare edges of the rocks are often exposed 
 over the intervening ridges from creek to creek. Well-marked beds of interstratified 
 conglomerates seem to retain their character over large areas, and the loose pebbles 
 from these can be followed readily over the ridges, whilst the rock from which these 
 pebbles are derived crops out in the gullies and ravines.” 
 
 I had an opportunity of visiting this interesting locality in October, 1886, and 
 traversed the river for about ten miles above the crossing of the road from Pentland to 
 Gilberton. The strata strike north-east and south-west, and dip on the whole at high 
 angles to the north-west. In the first mile above the crossing there is, however, first a 
 synclinal trough and then an anticlinal arch, so that the outcrops of some of the strata 
 are seen three times. Allowing for this repetition, the following section Gn descending 
 order) can be made out :— 
 
 
 
 Feet. 
 1. (Ten miles up the river.) Hard grey or white and yellowish sand- 
 stone, sometimes weathering spheroidally, alternating with 
 soft, thin, grey shales ssa : aoe oA Sea opr td) 
 2. Soft, thin, grey shales (vertical: ee N. 35° E. aS ne ... 1,000 
 3. Soft, grey, sandy shales or argillaceous sandstones, sometimes 
 calcareous, and containing Corals, Crinoids, and Brachiopods 
 (nearly vertical: strike N.E. and S.W., marked cleavage- 
 planes, dipping to N. at 15° to 25°) e. aie me ion, 1;000 
 No section—room for... «ay 2 BOD 
 4. Limestone (strike N.N.E. to 8. S. W. aye ened for Gro ey ile UD 
 5. Shales ses vic ye be ¥ ee sh ea 
 6. Fine Sonplomierates, iss aa ae ee dive Rote 
 7. Limestone ... ie ie At i sae ar = sas 50 
 Carried forward ... Ses ee fey. a ee ars | 0,000 
 
 
 
 * Quart. Journ. Geol. Soc., vol. xxviii., pp. 290, 291. 
 
37 
 Feet. 
 Brought forward AQ Sire ... 8,630 
 8. Coarse conglomerate (pebbles up one foot | in ldiameter): pebbles of 
 granite, porphyry, diorite, quartz, quartzite, hardened sand- 
 stone, and Jydian stone (vertical: strike N.N.E. toS$.S.W.) ... 2,640 
 9. Limestone, full of Crinoids and Corals, alternating with fine-grained, 
 
 greenish-grey sandstones, and shales, seen at intervals os PU) 
 
 10. Shales, sometimes calcareous ... a Oe 
 11. Limestone, in parts an agglomerate of coral houlders, with partings 
 
 of grey shale oa sink ee a 
 
 12. Shales, with thin beds of Trieatone A ntervale as ir soa USAW 
 
 13. Limestone.. ro a3 eet we aus ae ae etal OOO 
 
 14. Shales... oe 20 
 
 15. Fine-grained, dark- blue, Foalesreous pendent in thin fede yt 30 
 
 16. Shales, seen at intervals 100 
 17. Limestone, in thin beds, full bE Corals Cravnsiive, Treitonign, &e.) 
 
 and Crinoids (strike N.N.E., dip N.N.W. at 75°)... 3 12 
 
 18. Dark grey-green, crumbling slates or shales, seen at intervals... 600 
 
 19. White grit 1a oe ~ ay hd Sr re fk 20 
 
 20. Limestone (coralline) .., ava 5 ihe ies id en GOO 
 
 No section—room for .,.. “3 sd adi ase ee «sw», 600 
 
 21. Limestone (coralline) .., dein ae ~~ reer ne 0.8) 
 
 22. Fine quartz-conglomerate or pebbly sat ss 30 
 
 23. Conglomerate, pebbles chiefly of sandstone up to” six jones in 
 diameter, reddish matrix (strike N. 30° E., dip W. 30 N. 
 at 70°) Son Sh os oe = ce ee et 50 
 24. Slate, seen at intervals ... +i os 100 
 25. Quartz-conglomerate; the upper part has pebbles of har dened: fue: 
 } grained, grey ¢ and greenish sandstone as well as quartz, with 
 partings of grit and shale (strike N.N.E., dip N.N.W. at 70°) 400 
 
 : 26. Slates and greenish-grey flags, seen at intervals (strike N.N.E., 
 dip N.N.W. at 75°) ee = 1,320 
 
 27. Thick-bedded, hardened, grey and precnish siliceous grits, with 
 shale partings (strike N.E., dip N.W. at 70°) a ' 100 
 
 , 28. Thick-bedded, hardened grey aa greenish siliceous grits (strike 
 : N. and S., vertical) ae 200 
 
 29. Green, decomposed, fine-grained, wauuee metimorphic oer. 
 passing into contor ea green slate or schist (vertical: strike 
 
 ; N.E. to S.W., dipN.W.)... ws. 2,640 
 30. Coarse altered grit containing eevaihld of felspar and homblende 2,640 
 31. Hardened white sandstone, almost quartzite ; - 100 
 32. Thick-bedded, hard, white siliceous sandstone taike E. N. E., dip 
 
 NOIN Ws at.7o le ws, ' 50 
 33. Conglomerate ; pebbles, hard aite siliceous sandstone and 
 quartzite, a few slate, and a very few of quartz ef °F 30 
 No section—room for ,., He x oe re 50 
 34, Thick-bedded, hardened, white siliceous sandstone = oe LOU 
 No section—slates seen at intervals—room for... pe <a + 160 
 35. Blue slates and sandstones (dip N.N.W. at 60°), say Ag 2, POU 
 No section—room for ... iz & eae see eek ag) © 800 
 36. Fine-grained, blue, slaty sandstone ... : 100 
 37. (At road crossing.) Blue slates Se W. at 20°, clea ae NN, E. 
 and §.W.) ... ina 0 De ah Ar 24 ae 800 
 38. Coarse conglomerate... ~ igs i ee te cea LOD 
 
 
 
 20,782 
 
 
 
38 
 
 Away from the river the two beds of limestone, Nos. 20 and 21, are separated by 
 a hollow (denoting the prevalence of soft rocks, probably shales), in which débris of 
 shale or slate, and lumps of manganese oxide and hematite, can be seen in the soil. 
 Both beds of limestone are covered on the top with bottle-trees. These beds cross 
 the road about three miles north of the river, and contain numerous caves, in some of 
 which gold has been obtained on washing the detritus on the floor. 
 
 As the whole of the strata comprised in the above section are evidently part of 
 an unbroken series, and the limestone beds have, from their fossil contents, been 
 identified with those of the Burdekin Beds, the whole thickness (20,782 feet) must be 
 considered as belonging to the same division of the Devonian rocks. How much more 
 would be added to this by foilowing the Broken River down to its junction with the 
 Clarke, I cannot say. 
 
 From the Broken River the Pentland and Gilberton road runs north-west to 
 McKinlay’s (twenty miles). Two miles beyond the ‘‘ Limestone Wall”’ (bed No. 20 in 
 the above section), the road crosses soft, white, yellow, greenish, and liver-coloured 
 sandstones, with partings of grey and occasionally liver-coloured shales ; then a six-feet 
 bed of limestone-conglomerate, containing pebbles of limestone (chiefly), sandstone, 
 and conglomerate, in a limestone matrix. The limestone pebbles are masses of coral. 
 This singular conglomerate strikes north-north-east to south-south west, and is succeeded 
 to the north-west by red shales. For the next mile the road crosses grey sandstones, to 
 which several thin beds of limestone succeed. Thence to McKinlay’s the road crosses 
 gritty yellow sandstones. 
 
 About a mile north of Pandanus Creek (on which McKinlay’s Station is situated) 
 is a thick bed of limestone, said to be traversed by an antimony lode. From 
 McKinlay’s north-west for about cight miles (across the divide between the Burdekin 
 and EHinasleigh waters) the road crosses several beds of limestone alternating with 
 brown and white sandstones and red shales. After seventeen miles more, in which no 
 strata crop up on the road, basaltic rocks are met with, which continue for at least fifteen 
 miles more to the Lynd Station, on Lee Creek, a tributary of the Hinasleigh. It is 
 probable that the basalt overlaps the stratified rocks just described. 
 
 The whole of the stratified rocks, which include several beds of limestone, met 
 with along the road north-west of the Limestone Wall in all probability belong to the 
 same series as the limestone in the wall itself. Some of the sandstones and liver-coloured 
 and greenish shales remind one strongly of the shales above the Fanning Limestone. 
 
 In returning, in December, 1886, to Townsville from the Croydon Gold Field, 
 vid Georgetown, I took the direct road from the Lynd Station to Townsville, which 
 crosses the Clarke River at the Telegraph Station near its mouth. Eight miles from 
 the Lynd Station the basalt country comes to an end. In two miles more the divide, 
 here almost imperceptible, between the Hinasleigh and Burdekin waters is crossed. 
 Granite is seen on the road for the next three miles. To the granite succeed twelve miles 
 of mica-schist country, with numerous quartz reefs. After two miles of basalt the valley 
 of Paddy’s Gully is reached. The gully is in mica-schist, which extends along the 
 road half-a-mile on either side of the gully. Then comes half-a-mile of stony basalt 
 country ; then two miles of mica-schist and two of basalt; thence to two miles short 
 of Gray Creek (five miles) mica-schist is met with. I regard the mica-schists met with 
 between this point and the divide as of an older date than the Broken River Limestone 
 and associated strata. 
 
 At the point (two miles short of Gray Creek) where the mica-schist is seen for 
 the last time, strata similar to those on the Pentland road, north-west of the Limestone 
 Wall, are met with. The first eight miles are over red shales, partly jasperised. As far 
 
=o! eS — 
 
 a a ee ee es 
 
 39 
 
 as Doughboy Creek (sixteen miles) the road crosses highly inclined brown and yellow 
 sandstones. Near Doughboy Creek these beds are overlaid unconformably by tablelands of 
 Desert Sandstone, which extends south-westward nearly to the Broken River. For the 
 next six miles, to Christmas Creek, the road traverses brown and yellow sandstones, 
 grits, and conglomerates. Near Christmas Creek amygdaloidal porphyrite is seen on 
 the road, but its relation to the sandstones, &c., could not be made out. Beyond this 
 point the setting in of the wet season made further geological observations impossible, 
 so that I am unable to say how far the Devonian rocks extend to the east of the Clarke 
 River. 
 
 The strata seen on the Townsville road nearest the mica-schists, it must be remem- 
 bered, are high up in the Devonian Series. They therefore, probably, do not in this 
 locality overlie the mica-schists, but are most likely divided from the latter by a fault. 
 
 Referring again to the section seen on the Broken River, it will be observed that 
 the thick limestone, No. 20, is the lowest bed in which I have actually observed the 
 occurrence of fossils, although the time at my disposal was far too limited to admit of 
 a careful search. Tor eins! therefore, that can be proved to the contrary, the 
 underlying beds, which have a thickness of 10,000 feet, may pass downward into the 
 Lower Devonian or even Silurian. But no such division can be made without positive 
 evidence, and as the whole section of 20,782 feet forms an unbroken series it must for 
 the present be regarded as Middle Devonian. 
 
 When the “ Handbook of Queensland Geology ’’ was published, I was under the 
 impression that the strata above described as lying on the Fanning Limestone were the 
 equivalent of the “ Dotswood Beds” in the Keelbottom Valley, and that both were on 
 a lower horizon than the “Star Beds.” ‘The “Star Beds” form the lowest member of 
 the Permo-Carboniferous Series, and therefore are, probably, most nearly related homo- 
 taxially to the European Carboniferous.* More recent observations have shown (1st) 
 that the ‘ Dotswood Beds” and the ‘‘Star Beds” are identical; and (2nd) that the strata 
 lying above the Fanning Limestone are the equivalents of similar strata which overlie 
 the Broken River (Middle Devonian) Limestone, and with which thin beds of limestone 
 containing the same fossils as the Broken River Limestone itself are intercalated. The 
 strata above both the Fanning and the Broken River Limestones are now regarded as 
 belonging to the same formation as these limestones, and as there can be no passage 
 from Middle Devonian into Carboniferous, the “Star Beds,” with which the ‘‘ Dots- 
 wood Beds” are now united, must be unconformably related to the former. 
 
 Part of this area is further described by Mr. Maitland in his Report on the 
 Geology and Mineral Resources of the Upper Burdekin,t as follows :— 
 
 “The series of strata classed under this head [Burdekin Beds] occupy a very 
 extensive tract of country. 
 
 “The basin is bounded on the west by a belt of schistose rocks of variable width, 
 and on the north and west by the granitie rocks which make up the main coast range. 
 Small patches of schistose rocks, however, are seen near the tin lodes at Kangaroo 
 Hills, separating the Burdekin Beds from the granite, but of too small an area to be 
 shown on the map. 
 
 “Tn their lithological characters they present a marked contrast to the rocks 
 above and below them. The strata consist for the most part of dark-buff and reddish 
 
 
 
 *Tt is probable that the ‘‘ Star Beds” are the equivalent of what in New South Wales are at present 
 known as the ‘‘ Lower Carboniferous,” but which, it is anticipated, will in future be regarded as the nearest 
 representative of the Carboniferous of Europe. These I have now termed Carboniferous in the New South 
 Wales Classification. (See Mem. Geol. Survey, N.S. Wales, Pal. Series, No. 5, pt. 1, 1891, p. 3.—R. £. aie ) 
 
 + Brisbane: by Authority : 1891, p. 4, 
 
40 
 
 coloured shales, sometimes jasperised, together with grits, greywackes, and quartzites 
 generally inclined at high angles. The thickness of these beds, unless repeated by 
 folding, must be very great. 
 
 “From their lithological characters it appears possible to divide them into two 
 subdivisions, one consisting for the most part of reddish shales and ferruginous 
 chocolate-coloured sandstones, and the lower of dark shales, grits, and greywackes. 
 From the fact that these reddish beds were first seen near Wairuna Station, for 
 convenience of description I have named them the Wairuna Beds. 
 
 “From the Four-mile Creek—a tributary of the Douglas—to Kangaroo Hills 
 Station the gullies show buff-coloured vertical shales and greywackes, striking generally 
 east and west. 
 
 “The eastern bank of the river at Kangaroo Hills Station is composed of buff 
 shales and greywackes, which dip at an angle of 80° N. 70° W., and strike N. 30° E. 
 
 “Near the tin lodes, the ‘Star Beds’ are seen to rest upon a series of highly 
 inclined hardened grits and shales. In close proximity to the granite, beds hardened 
 and metamorphosed are met with; to ascertain whether these are representatives of the 
 Burdekin Beds more highly altered, or are of older date, would require much more 
 detailed work than is possible in a flying reconnaissance. 
 
 “From Kangaroo Hills Station to the mouth of Camel Creek the country is 
 occupied by vertical shales of a somewhat similar type to those above described. In 
 Tomahawk Creek they strike W. 20°S. Between this pomt and the crossing of the 
 Douglas the sedimentary strata are intersected by a tongue of granite. 
 
 “From the mouth of Camel Creek to a gully about 2 miles further down the 
 river the country is made up of vertical contorted shales and greywackes; at the south 
 end of the section their strike is north and south, at the mouth of Camel Creek it has 
 veered round to west-north-west. 
 
 “A few low hills of flaggy grits, dipping at angles of from 25° to 30° to the north- 
 wards, are passed over in traversing the country from the mouth of Camel Creek to a 
 point on the opposite side of the Burdekin to Greenvale Station. 
 
 “To the Valley of Lagoons Station comparatively few sections are to be seen, 
 owing to extent of flat country covered with recent superficial deposits. At one place 
 about 5 or 6 miles north of Greenvale Station, ridges showing vertical sandstones 
 striking north-east and south-west occur. These bear a strong lithological resemblance 
 to those last described. Similar beds underlie the flats for the next few miles, then their 
 place is taken by reddish jasperised shales. The relation of these shales to the sandstones 
 is not very clear, but I am inclined to regard them as being separated by a fault. 
 
 “ Further northwards along the road the eye is attracted, even at a distance, by a 
 conspicuous cliff about 100 feet in height. On nearing it the western face was found 
 to be full of caverns of no great size, and the base was strewn with huge boulders of 
 rock. The matrix of which this hill is composed is a quartz rock generally with a 
 reddish tinge, though sometimes white. It appears to be bedded, the bedding planes 
 being nearly vertical and striking north and south. Some of the weathered surfaces 
 suggest a volcanic origin (ash ?). 
 
 “Underlying the flats of the next mile or two are shales, &c., dipping at 25° to 30° 
 to the north-east. 
 
 “The country to the east of the station at the Valley of Lagoons is occupied 
 by fine-grained sandstones of a yellowish-brown or buff colour. In some places the 
 sandstones are crowded with sun-cracks. They rest unconformably upon the schists, 
 and dip to the south-east at angles varying from 70° to 30°. They do- not form any 
 important feature in the landscape. 
 
ae | > J——- 
 
 41 
 
 “In the vicinity of Wairuna Station, vertical shales of a reddish-purple colour 
 strike north and south, some of which look not unlike fine voleanic ashes. At one place 
 west from the station some of the shales are found to be associated with thick beds of 
 quartzite ; these strike north-east and south-west. The Wairuna beds are seen cropping 
 up at intervals along the track to Lake Lucy Station. 
 
 “The environs of Lake Lucy are made up of reddish clayey shales, identical 
 with those above described, and having the same general trend—viz., north-east and 
 south-west. Interstratified with these shales are bands of limonite intermingled with 
 veinlets of quartz. These bands are not continuous for any distance. All of these 
 examined were parallel with the bedding planes, and of very variable thickness. A few 
 quartz reefs intersect these shales. Between Lake Lucy and Oak Hills, the Wairuna 
 Beds occupy the country ; they retain the same character and strike. Unless repeated 
 by faulting and folding (which is not improbable) these Wairuna Beds must be of 
 enormous thickness. 
 
 “Among the rocks above described there may be beds which future detailed 
 mapping may prove to belong to other systems. 
 
 “At present, in the absence of paleontological or stratigraphical evidence, the 
 whole beds are provisionally classed as belonging to one system.” 
 
 The hill to the north of Torrent Creek, on the western side of the Reid Gap, is 
 capped by a stratified deposit. The lowest strata are of limestone, of a total thickness 
 of about 60 feet, divided by occasional thin layers of hardened sandstone. The 
 deposit varies in quality from top to bottom, some strata being dark-blue limestone, and 
 others white saccharine marble. Some of the blue beds are full of fossil corals. 
 Above the limestone is a thickness of about 40 feet of hardened grey mudstones with 
 calcareous bands. The strata on this hill-top dip N. 30° E. at about 25°. 
 
 The hill on the opposite or eastern side of the Gap is likewise composed of 
 stratified deposits, as follow :— 
 
 Feet. 
 1. Hardened white sandstone or quartzite partly conglomeratic ... ote 
 2. Sandstone (thickness uncertain) ae Bc is cm a 
 3. Good blue limestone with corals, say ee . 30 
 4. Hard mudstones and fine-grained har dene “gandstones: “(almost 
 quartzites), with limestone in bands ed aie planes ns 230 
 
 5. Good blue limestone (base concealed by talus) . 
 
 The strata numbered 4 and 5 in the above section are the same as those already 
 described as capping the hill on the opposite side of the valley. The limestone at the 
 base of the section last given lies directly on granite. 
 
 On the hill-tops west of the railway at Double Barrel Creek, the following strata 
 dip to the south-west, and rest unconformably on greywackes, &c., probably of the same 
 age as the stratified rocks west of Charters Towers :— 
 
 Feet. 
 Dark-blue limestone, full of corals; the lower part gs divided id) 
 partings of quartzite, at least .. ; 200 
 Alternate quartzite, limestone, and marble bands, say . ae ee Ohne 
 Blue greywacke a ' val is x Pe oe 13 
 Alternate quartzite and limestone bands . ss sis ass ef 40 
 Dark-blue greywacke ee ee at ro ee e, Fe 5 
 Scrub, perhaps covering are =: a. ee er BAG =i6 20 
 Limestone with quartzite bands... me Fc at a a AY) 
 Fine-grained dark-blue greywacke .. ie i mi ae aes 4 
 Impure saccharine marble, with dark streaks a ats nee es 15 
 Dark-blue coraljine limestone, about ee se =H “ owe 60 
 
42 
 
 In the neighbourhood of Clermont a bed of dark crystalline limestone crops out close 
 to Douglas Creek, about three miles below its junction with Drummond Creek, and about 
 four miles south-east of Copperfield. The limestone is full of corals, among which Mr. 
 Rands recognised Fuvosites, Chetetes, Cyathophyllum, a compound cyathophylloid resem- 
 bling Strombodes, and Stenopora (?), together with a fragment of a Lamellibranch shell.* 
 
 In Marble Island, in the Northumberland Group, a limestone is extensively 
 quarried. In some cargoes of this limestone I have seen corals of the species which 
 characterise the Burdekin Beds. 
 
 In 1887 I had an opportunity of visiting Hunter Island, which lies about half- 
 a-mile west of Marble Island, in Lat. 21° 58’ S. and Long. 149° 9’ E. The island 
 extends from north to south about a mile and a-quarter, and has an average breadth of 
 less than a quarter of a mile. It is well grassed, but the timber is confined to a few 
 trees on the beach, among which are some hoop pines. The southern portion of the 
 island is joined to the northern by a narrow neck or isthmus, and is wholly composed of 
 granite. In the bay, on the eastern side of the neck, and in the wide portion of the 
 island to the north, a series of stratified rocks make their appearance. They have a 
 north-and-south strike, and dip to the east at 65°, being, in all probability, divided by a 
 fault from the granite on the south. The uppermost (easternmost) bed seen is a white 
 marble at the north end and a blue limestone at the south. Below this, to the west, 
 comes a considerable thickness of highly contorted shales or slates, with seatas, nodules, 
 and lenticular patches of coralline limestone. Next comes a thick bed of blue lime- 
 stone, which graduates northward into pink marble. Sandstones and conglomerates 
 underlie the bed last mentioned, and are best exposed in the bay on the east side of the 
 isthmus. The last and lowest bed seen is at least 100 feet in thickness. On the east 
 side of the isthmus it is an ordinary blue limestone. On the edge of the bay to the 
 north, its upper part is white and its base a pink marble. Considerations of wind and 
 tide made my visit to the island, in spite of the time consumed in reaching it, a very 
 short one, and I had no time to search for fossils. Thereis no reason to doubt, however, 
 that the limestone and other stratified rocks of Hunter Island are of the same age as 
 the limestone of Marble Island. The northern end of Marble Island is composed of 
 limestones, &e., and the southern end of granite, so that it is probable that here, as in 
 Hunter Island, the stratified and plutonic rocks are divided by a fault. 
 
 It is noticeable that the northern portions of the outcrops of the three large beds 
 of limestone in Hunter Island have become changed from the usual type of blue-grey 
 limestone into marble. There is no visible cause for this development of “ regional 
 metamorphism,’’ but it is likely to be due to deep-seated igneous rocks or hydrothermal 
 action. As the limestones, &c., were laid down subsequent to the formation of the 
 granite, and, where seen, at the southern part of the isthmus, in closest proximity to it, 
 are quite unaltered, it is evident that the latter can have bad nothing to do with it. 
 The western half of the northern portion of the island is composed of granite like its 
 southern extremity, and it is probable that the stratified rocks were deposited on the 
 granite long subsequent to its consolidation. A mass of diallage-rock is seen on the 
 western shore of the island, apparently intrusive through the granite. 
 
 The limestone, of which there is an unlimited quantity, would serve, admirably 
 for a building stone or for the manufacture of lime. Some argillaceous portions 
 would make hydraulic lime. The marble is minutely crystalline and pure white, and 
 quite fit for ornamental architecture or statuary. What I have above alluded to as 
 “pink” marble is a very beautiful stone suffused with a faint blush-rose tint. 
 
 
 
 * Report on the Geology and Mineral Deposits of the Country in the Vicinity of Clermont, Brisbane; 
 by Authority: 1886, p. 4. : 
 
43 
 
 In the following list of fossils from the Devonian rocks of Queensland, all are 
 included which my Colleague has recognised or admitted. The species are distributed 
 among the four localities from which collections have been made, but these localities are 
 practically on the same horizon. 
 
 SYSTEMATIC LIST OF MIDDLE DEVONIAN FOSSILS. 
 
 
 
 
 
 Broken R. 
 Fanning. 
 Burdekin. 
 
 Reid. 
 
 
 
 
 
 Kingdom—PLant x. 
 Section—PHANEROGAMOUS PLANTS. 
 Class—Exocun a. 
 ? Order—CoNIFERR. 
 Genus—DiIcrRANOPHYLLUM, Grand ’Kury. 
 Dicranophyllum australicum, Dawson Age 508 ae 596 ao ||). oor x 
 
 
 
 Kingdom—ANIMALIA. 
 Sub-Kingdom—C@LENTERATA. 
 Class—HypDROzOA. 
 Order—HYDROCORALLIN ®. 
 Family—STROMATOPORID®. 
 Genus—StTRoMATOPORA, Goldfuss. 
 Stromatopora, sp. ind., Pl. 1, figs. 3-5 Ge 500 aoe aes a0 x nc x x 
 
 Class—AcTINOzOA. 
 Order —ZOANTHARITA. 
 Sub-Order—Z,. ScLERODERMATA. 
 ' Section—PERFORATA. 
 Family—Favositipm. 
 Genus—F avosires, Lamarck. 
 Favosites gothlandica (Fougt.), Lamarck ... on sn see 56 x 
 Genus—Pacuyrpora, Lindstrém. 
 Pachypora meridionalis, N. & H. fil. ... or te “i on, abo. ace x x x 
 Genus—ALVEOLITES, Lamarck. 
 Alveolites alveolaris, De Koninck, Pl. 2, figs. 1-3 ee ave 
 As ee Var. queenslandensis, Eth. fil. and Foord, sed. 2, 2 figs. 4 4 6 ae Sor Hf: 
 robustus, Rominger, Pl. 1, figs. 13,14 ... ee ia Se 
 sp. ind., Pl. 1, figs. TSENG As eae sae aa pn eee Waele we x 
 Genus—-AMPLEXOPORA, Ulrich. 
 Amplexopora (?) Koninekii, Eth. fil. and Foord, Pl. 2, figs. 7-9a ... Shad) ah ae Nise x 
 Genus—TrRracnypora, Hdw. and Haime. 
 . Trachypora, sp. ind.,N.and EH. fil. ... Rae sa ai Bot foals ee wee x 
 Genus—StTRIATOPORA, Hall. 
 ; Striatopora (?) uniseptata, Eth. fil. ... “ins sare So avs Sobel! Bed x 
 Genus—RomincGertaA, Nicholson. 
 Romingeria (?) Foordi, Eth. fil. as Ase nef or ae sent | eee Sut jon x 
 Genus—C@niteEs, Hichwald. 
 Cenites, sp. Bon aie ne ser Sa nae Sa are ae ope 
 
 x x 
 
 ” 
 
 
 
 
 
 jm oemat 
 
 Family— Poritip®. 
 Genus—Armopora, N. and FE. fil. 
 Areopora australis, N. and HE. fil., Pl. 3, figs. 6-9 ate: ae Ag Scoalh on Rep x 
 
 pap 
 
 Section—Ruaosa. 
 
 Family—CystIPHYLLID®, 
 
 Genus—CystirpHyLiumM, Lonsdale. 
 Cystiphyllum americanum, Edw. and Haime, var. australe, Eth. fil.,| ... es as x 
 d Pl. 3, figs. 13, 14 
 
 Genus—CYATHOPHYLLUM, Goldf. 
 Cyathophylium, sp. ind., Pl. 3, figs. 11,12... woe S60 wate cia eee her ane x 
 
 
 
44. 
 SYSTEMATIC LIST OF MIDDLE DEVONIAN FOSSILS—continued. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 oT eee 
 4 a 3 3 
 = # E 8 
 a) A a) =) 
 Family— ZAPHRENTIDE. 
 Genus—AmPLexts, J. Sowerby. 
 Amplexus, sp. ind., Pl. 37, ‘figs. 15, 16.. 356 " tee . “ x 
 Genus—CAMPoPHYLuM, Edw. and Haime. 
 
 Campophyllum Gregorii, Eth. fil., Pl. 3, figs. 15-18 ... ant ieee Se ico |b. oar ny Bot x 
 
 Order—ALOYONARIA. 
 Family—HELIoLiItip®. 
 Genus—Hertiourres, Dana. 
 Heliolites porosa, Goldf., Pl. 1, fig. 6 
 a Daintreei, Eth, fil. and Nich., Pl. ib ‘figs. 7, gees 
 x plasmoporoides, Eth. fil. and Nich. oat il figs. 9-11 
 Rs Nicholsoni, Eth. fil., Pl. 1, fig. 12. 6 
 
 x XX X 
 
 Family —AvLoporip2. 
 Genus—AULOPORA, Goldf. 
 Aulopora repens, Edw. and Haime 
 0 sp. ind. 
 
 wae wee eee ane tee eee eee eee eee 
 
 
 
 Sub-Kingdom—EcnInoDERMATA. 
 Section— PELMATOZOA. 
 Class—CRINOIDEA. 
 Order—PALEOCRINOIDEA. 
 Crinoid stems ae ie ae 58 aac aad 6 Be x 
 
 Sub-Kingdom—Mottvsca. 
 
 Class—BRACHIOPODA. 
 
 Order—TRETENTERATA. 
 
 Family—SpirireRiIpm. 
 
 J. Sowerby. 
 
 Spirifera curvata, Schlotheim, Pl. 37, figs. 3-5, 7 ©... See 2s 
 55 euryglossa, Schnur, Pl. 4, fig. 1... “be 
 
 
 
 x 
 
 Family—ATRYPIDE. 
 Genus—ATRYPA, Dalman. 
 Altrypa reticularis, Linneus, Pl. 4, fie Ae ies ac 5b tf sos ih onc 
 a desquamata, J.deC. Sowerby, Pl. 4, figs. 2,3; Pl. 37, fig. 8 
 
 x xX 
 
 
 
 Family—RuYNCHONELLID®. 
 
 Genus—RHYNCHONELLA, Fischer. 
 Rynchonella primipillaris, von Buch., Pl. 4, fig. 5 ... 
 
 Genus—PENTAMERUS, J. Sowerby. 
 Pentamerus brevirostris, Phillips, Pl. 37, figs. 6, 9-11 
 
 Family—StTRin@ocEPHALID®. 
 
 Genus—StRInGocrernalvs, Defrance. 
 
 Stringocephalus ? sp. ind. : a nee cat nr = Ri abs ss 
 Family—STRopHoMENID ®. 
 Genus—OrTHOTETES, Fischer. 
 
 Orthotctes umbraculum, Schl. 
 
 a5 ? concentrica, Eth. fil. 
 
 Class—CEPHALOPODA. 
 Order—TETRABRANCHIATA. 
 Family —NAvTILIDm. 
 Genus—GyYroceras, De Koninck. 
 Gyroceras Philpi, Eth. fil., Pl. 4, figs. 6,7 ... a bat ale Det Maes x 
 
 ne 
 
a 
 
 i 
 « 
 » 
 
 
 
 45 
 
 In the above list we have a fairly representative collection, with a decided pre- 
 ponderance of Middle Devonian forms. It will be seen that not a single fossil hitherto 
 collected is specifically identical with any which are known in the Permo-Carboniferous 
 System. Three genera of Actinozoa, viz., Fuvosites, Pachypora, and Oyathophyllum, 
 and two of Brachiopoda, viz., Spirifera and Rhynchonella, are, however, repeated in the 
 Gympie Formation ; and the two Brachiopods above named are also repeated in the 
 Star Formation. Sp7rifera alone survives in the Middle Bowen Formation. 
 
 The Queensland Devonian may be fairly placed on the same horizon as the 
 Middle Devonian Limestones of Bindi and Buchan, Victoria,* and is probably on a 
 lower horizon than the Upper Devonian of Tynana Creek, Victoria. My Colleague 
 informs me that the Lower Devonian age ascribed to various rocks in New South 
 Wales is doubtful, and that all the fossils from these rocks which have come under his 
 notice are now believed to be Upper Silurian. 
 
 MINES IN CONNECTION WITH THE MIDDLE DEVONIAN ROCKS. 
 ARGENTINE SILVER FIELD. 
 
 The argentiferous lead lodes of the Argentine Field occur partly in granite 
 country and partly among highly inclined micaceous clay-slates, mica-schists, and 
 gneisses. Regarding the age of the sedimentary rocks above referred to, no distinct 
 evidence has yet been brought to light, but from their position between the Broken 
 River and Reid, they may be supposed to be continuous with the Middle Devonian 
 rocks of these districts. A thick series of white sandstones, pebbly grits, and 
 conglomerates, probably identical with the lower portion of the Star Formation, lies 
 unconformably on the slates, &c., or rests on the granite. 
 
 The field has been in existence since 1881. The lodes, especially those in the 
 mica-schist country, offer every indication of richness and permanence; fuel and 
 limestone and ironstone for fluxing are abundant and conveniently situated. In spite 
 of all these advantages, prosperity has hardly yet dawned on the field. The majority 
 of the lodes were originally secured as freeholds under the old Mineral Lands Act, the 
 workings being for a time of a very perfunctory nature and having for their object 
 the bare fulfilment of the “improvement conditions,’ or the raising of sufficient 
 specimens to induce outsiders to purchase the mines, Some of the mines, worked 
 on a “poor man’s” scale, have obviously failed through the mechanical difficulty of 
 separating earthy low-grade oxide and carbonate ores from the almost equally heavy 
 ferruginous gangue-stuff without dressing machinery. The failure of the smelting 
 works, which were erected prematurely, before sufficient quantities of ore were ready 
 for them, was a severe blow, destroying as it did confidence in the value of the mines, 
 and bringing about their almost complete desertion. The Hero and Northbrook Mines 
 have, however, been steadily worked at a profit for some years, the ores being shipped 
 from Townsville. The Hero has recently been taken up by a Sydney company. 
 
 The surface ores, which have alone been raised hitherto, consist for the most 
 part of oxides, carbonates, sulphates, and sulphides of lead. The silver contents of 
 samples which I have assayed average generally about 14 oz. per ton to the unit of lead, 
 but occasionally reach 5 oz. of silver to the unit. In other words, a ton of galena ore 
 containing 60 per cent. of lead might contain from 75 oz. to 300 oz. of silver. 
 
 There can be no doubt that this field will yet take a high place among the 
 silver-producing localities of Australia. * 
 
 *Geology and Physical Geography of Victoria, by Reginald A. F. Murray. Melbourne : by 
 Authority : 1887, p. 53. 
 
46 
 
 As the Argentine Field was only occasionally visited by the Warden from Ravens- 
 wood, the returns of the output as given in the Annual Reports of the Department of 
 Mines only give occasional references to quantities of ore exported. The following are 
 all the particulars obtainable from this source :— 
 
 1883 
 1884, 
 1885 
 1887 
 1888 
 1889 
 
 10 tons exported Value, £20 
 
 20, Fs Aon AC ie 225 
 20 ,, ae. » 600 
 40 ,, produced .., AOE * 680 
 5015; < fs Ae ee L000 
 76 ,, %» ue os » 8,804 
 
 Three exporters of ore have supplied me with the following returns of ore which 
 passed through their hands during a portion of the time covered by the existence of 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 the field :— 
 ASSAY, 
 Date. Exporters. Quantity of Ore. ee ere 
 Lead. Silver. Gold. 
 Tons ewt. qr. 1b. ee s. d.| Percent. |Oz. per ton.|Oz.per ton. 
 
 May, 1883... | L. Ryan Sy MMO) Oe CO) || aalss (0) 60) - 
 May, 1887... Ditto LOR OmnO op) 10) 0 
 Jan. 1, 1884 
 
 to Hays and Bundock 200 O 0 011,600 0 0 
 Jan. 1, 1888 
 June, 1885... | Allen and Sons* .., 3 By OF @ 39 8. 0 101:26 | 0327 
 July, 1885... Ditto Be LomsOmno) 46 0 0O ae 98 0°337 
 Aug., 1885... Ditto 6 14 2 26 3 OO 30 60°43 1:47 
 June, 1886... Ditto OM 1be 0 Oni alos Om O 43 84: SHC 
 May, 1887... Ditto 3 tay a ae 20 OO 43 85 
 June, 1887... Ditto Le ORLG ive AG) 33 64: 
 July, 1887... Ditto Gitone Zee 2716 O 20 57 
 Aug., 1887... Ditto ATES O SO 2116 O 64 27 
 Dec., 1887... Ditto DT LOOM 8 4 3 21 41 
 Jan., 1888... Ditto 3) ia ah 1211 4 22 53 
 
 Totals 298 17 010/2,206 11 7 - 
 
 
 
 
 
 
 
 * Messrs. Allen and Sons’ returns give the amount received for the ore in England, less £1 per ton for freight. From 
 these I have deducted £4 per ton for carriage to port and other expenses. 
 
 J. 
 
CHAPTER V. 
 
 THE ORGANIC REMAINS OF THE MIDDLE DEVONIAN (BURDEKIN) 
 FORMATION, 
 
 With DEscrIprions OF THE SPECIES. 
 
 In the Devonian Series of Queensland there are at least four well-marked fossiliferous 
 horizons, the three last of which may possibly be merely extensions of one deposit. 
 They are :— 
 Limestones of the Broken River. 
 * » Burdekin Downs. 
 a » Fanning River. 
 », Reid Gap, near Townsville. 
 
 The Oyen Remains derived from the three horizons above named are almost 
 wholly corallian ; a few Brachiopoda from the Fanning Limestone, and one Cephaiopod 
 from the Reid Gap Limestone completing the list, it the exception of a plant— 
 Dicranophyllum australicum, Dawson—occurring both in a caleareous shale forming 
 the upper portion of the Fanning Limestone, and the lowest beds of the suprajacent 
 sandstone. 
 
 The Burdekin Downs Limestone has yielded :— 
 
 Stromatopora, sp. ind. 
 Pachypora meridionalis, N. and E. fil. 
 Alveolites robustus, Rom. 
 s sp. ind. 
 Trachypora, sp. ind. 
 Areopora australis, N. and E. fil. 
 Heliolites porosa, Goldf. 
 Aulopora repens, E. and H. 
 
 The Fanning Limestone has yielded :— 
 Dicranophyllum australicum, Dawson. 
 Pachypora meridionalis, N. and E. fil. 
 Striatopora ? uniseptata, Eth. fil. 
 Heliolites porosa, Goldf. 
 
 Spirifera curvata, Schl. 
 . euryglossa, Schuur. 
 Atrypa reticularis, Linn. 
 
 5,  desquamata, J. de OC. Sow. 
 Rhynchonella primipilaris, V. Buch. 
 Pentamerus brevirostris, Phill. 
 Stringocephalus ? sp. ind. 
 
 Orthotetes umbraculum, Schl. 
 f concentrica, Eth. fil. 
 
 Gyroceras Philpi, Eth. fil. 
 
48 
 
 From the Broken River Limestone we have :— 
 Stromatopora, sp. ind. 
 Favosites gothlandica (Fougt.), Lamk. 
 Heliolites porosa, Goldf. 
 S Daintreei, Eth. fil. and N. 
 x plasmoporoides, Eth. fil. and N. 
 m Nicholsoni, Eth. fil. 
 Amplexus, sp. 
 Crinoid stems. 
 The Reid Gap Limestone has yielded :— 
 Stromatopora, sp. ind. 
 Pachypora meridionalis, N. and E. fil. 
 Alveolites alveolaris, De Kon. 
 
 BS var. gueenslandensis, Eth. fil. and Foord. 
 Mipieeoneed ? Koninekii, Eth. fil. and Foord. 
 Romingeria ? Foordi, Eth. fil. 
 
 Cenites, sp. 
 
 Aulopora, sp. ind. 
 
 Cystiphyllum americanum, EB. and H., var. australe, Eth. fil. 
 Oyathophyllum, sp. ind. 
 
 Campophyllum Gregorit, Eth. fil. 
 
 Gyroceras Philpi, Eth. fil. 
 
 The age of these beds appears to be fairly marked out. ‘The Fanning River 
 Limestone and its associated shale have been shown to possess a strong claim to be con- 
 sidered Devonian. We have determined only two corals satisfactorily from this horizon, 
 Heliolites porosa and Pachypora meridionalis (nobis). The former, a typical Devonian 
 coral in Devonshire and the Eifel, supports the evidence afforded by the mollusea in a 
 marked degree ; that of the Pachypora will be considered immediately. 
 
 “We now come to the two localities, both in the Burdekin district—a limestone 
 developed on the Broken River and Arthur’s Creek, Burdekin Downs. The first point to 
 be noticed in connection with these localities is the presence of massive Fuvosites of the 
 Devonian type, quite undistinguishable from the F. gothlandicus and its variety F, 
 Goldfussi, of the Devonian of Europe and North America. Secondly, we note the 
 presence of numerous large colonies of Heliolites, including Heliolites porosa in 
 abundance. 
 
 “ Again, strong evidence of a Devonian age is afforded by the appearance here 
 of a coral which we cannot distinguish from Awiopora repens, Edw. and H., a very 
 characteristic Devonian species of the equally characteristic Devonian genus Trachypora; 
 while species of Alveolites of a Devonian type are also present. Hardly less characteristic 
 is the Pachypora to which we have given the name of P. meridionalis, and which is 
 most intimately allied to P. cervicornis, De Bla‘nv., sp., of the Devonian of Europe, and 
 to similar or identical forms in the Devonian of North America.”’* 
 
 Lastly, in the Reid Gap Limestone we again find Pachypora meridionalis and 
 Heliolites in abundance, together with Stromatopora, and the characteristic genus 
 Cystiphyllum, represented by a species of a markedly Devonian aspect, and other 
 Rugose corals indicating a similar horizon. ‘‘ Upon the whole, therefore, putting to the 
 evidence afforded by the corals, that derived from such characteristic forms as Stroma- 
 topora and Oaunopora, we cannot doubt that the deposits now under consideration are 
 
 * Nicholson and Etheridge junr., Ann. and Mag. Nat. Hist., 1879, vol. iv., p. 284. 
 
— 
 
 49 
 
 of Devonian age. So far as we are acquainted with their fauna, they would scem to 
 correspond very closely with the Middle Devonian Limestones of the Hifel, or perhaps 
 with the somewhat older series of the Corniferous Limestone of North America.’ In 
 other words, the series of rocks in question may be said to homotaxially represent those 
 formations. They are certainly not of Upper Devonian age, and there is no evidence 
 to assign them a position in the Upper Silurian. The Brachiopoda so far obtained 
 favour this view, and there is a marked absence of the large Pentameri, Strophomene, 
 and Crinoids which are usually the most marked objects in an Upper Silurian Fauna. 
 
 DESCRIPTION OF THE SPECIES. 
 Kingdom—PLANT&. 
 Section—PHANEROGAMOUS PLANTS. 
 Class—EXoGEN®. 
 
 ? Order—CONIFER#. 
 
 Genus—DICRANOPHYLILUM, Grand’ Eury, 1877. 
 (Mem, Acad. Sci. Inst. France, xxiv., p. 272.) 
 
 DiIcRANOPHYLLUM AUSTRALICUM, Dawson, Pl. 4, fig. 18. 
 D. wustralicum, Dawson, Quart. Journ. Geol. Soc., 1881, xxxvii., p. 306, t. 13, f. 15. 
 
 Sp. Char. The leaf bases are minute, narrow, elongate, and spirally arranged ; 
 the leaves are linear and bifurcating at an obtuse angle at their extremities. 
 
 Obs. This is the only plant yet found in the Devonian rocks of Queensland. 
 Sir J. W. Dawson appears to regard it as Corniferous. 
 
 Loc. and Horizon. Fanning River, Burdekin Downs, in a calcareous shale forming 
 the upper portion of the Fanning Limestone, and in white flaggy sandstone overlying 
 the same limestone. (2. L. Jack.) 
 
 Kingdom—ANIMALIA, 
 
 Sub-Kingdom—CC@iLENTERATA. 
 Class—HYDROZOA. 
 
 Order—HYDROCORALLIN &. 
 Family—STROMATOPORID. 
 Genus—STROMATOPORA, Goldfuss, 1826. 
 
 (Petrefacta Germanie, p. 21.) 
 Stromatoprora, sp. ind., Pl. 1, figs. 3-5. 
 
 Obs. Stromatopora occurred amongst Mr. Daintree’s fossils from the Broken 
 River Limestone, but in so highly silicified a state that a satisfactory examination of 
 the specimen could not be made. Another example has been forwarded by Mr. Jack 
 from the Arthur’s Creek Limestone, which is very like some Devonian species of 
 Devonshire and the Eifel. 
 
 Much more satisfactory and massive examples occur in the Reid Limestone, 
 enveloping the various corals which constitute that rock. Prof. H. A. Nicholson, 
 M.D., who was kind enough to examine specimens, at one time believed them to be a 
 
 Pachystroma, allied to P. denswm, Nich. and Murie; but a subsequent inspection, since 
 D 
 
50 
 
 he has been engaged on his ‘‘ Monograph of the Stromatoporide,” has led him to regard 
 the masses in the Reid Limestone as more probably referable to Stromatopora proper, 
 and even allied to the typical and true S. concentrica, Goldf., and Stromatoporella 
 (Pl. 1, figs. 1, 2). The surfaces of many of these large masses from the Reid 
 Limestone present mammillary or button-shaped prominences, which have been left by 
 the process of weathering, possessing, however, the same structure as the general mass. 
 They may be merely the result of peculiar preservation, or they may be young examples 
 included in the older ones ; at any rate, so far as we can at present ascertain, they do 
 not appear to have any specific value. 
 
 Pending a detailed and proper description of the Hifel. and Devonshire forms of 
 Stromatopora,* I refrain from entering into details concerning these specimens, and 
 hope to be able to do so, with more satisfactory material, at some future date. 
 
 Loe. and Horizon. Broken River, a tributary of the Clarke River (The late R. 
 Daintree) ; Terrible or Arthur’s Creek, Burdekin Downs (R. LZ. Jack); and Regan’s, 
 Northern Railway, thirty-one miles from Townsville, Reid Limestone (R. L. Jack). 
 
 Class—ACTINOZOA. 
 
 The three groups of the Zoantharia, Aleyonaria, and Rugosa are represented in 
 the Devonian of Queensland—the first by the genera Favosites and Alveolites, &c., the 
 second by Awlopora, Amplexopora, &e., and the last-named by the genera Oyathophyllum, 
 Campophyllum, and Cystiphyllum. The examination of all these corals is rendered 
 difficult, as in the case of the Stromatoporoidea, by their highly altered condition. No 
 doubt a further examination of the localities mentioned will bring to light a much more 
 copious coral fauna than that here described. 
 
 Order—ZOANTHARIA. 
 
 Sub-Order—Z. ScLERODERMATA. 
 Section — PERFORATA. 
 Family—FAVOSITIDA. 
 
 Genus—FAVOSITES, Lamarck, 1816. 
 (Hist. Anim. sans Verttb., i., p. 204.) 
 
 Obs. Amongst the Queensland corals are two forms of Favosites only separable 
 by the size of the corallites composing the respective colonies. These are referred to 
 the cosmopolitan Favosites gothlandica, and its variety Goldfussi. 
 
 A single specimen of a massive Fuvosites with plenty of tabule was obtained at 
 Raglan, Port Curtis, by Mr. W. H. Rands. It is preserved in a light slate-blue 
 conchoidal limestone and has a strong Devonian aspect. The material was not sufficient 
 in quantity to permit of the preparation of sections for a specific determination. 
 
 
 
 FavosttEs GOTHLANDICA, (Fougt.) Lamarck, Pl. 3, figs. 1-5. 
 
 Favosites gothlandica, Lamarck, Hist. Anim. sans Verttb., 1816, ii., p. 206. 
 Calamopora gothlandica, Goldfuss, Petrefacta Germaniz, 1829, i., p. 78, t. 26, fig. 3 a-e. 
 Favosites gothlandica, Edwards and Haime, Polyp. foss. Terr. Pal., 1851, p. 232. 
 Favosites Goldfussi, Edwards and Haime, zbid. p. 235, t. xx., fig. 3 a, D. 
 Favosites gothlandica, Nicholson and Etheridge fil., Ann. Mag: Nat. Hist., 1879, iv., p. 209. 
 Favosites gothlandica, Nicholson, Tab. Corals Pal. Period, 1879, p. 46, t. i., figs. 1-6. 
 
 Obs. It will be convenient to consider the form with the smallest corallites 
 
 (Pl. 3, fig. 4), as the typical F. gothlandica, whilst that with the larger calices may be 
 
 * Now in course of preparation by Prof. H. A. Nicholson, and publication by the Paleontographical Society. 
 
gyi 
 
 ; 
 F 
 
 
 
 51 
 
 looked upon as the variety Goldfussi (Pl. 3, fig. 1). It has been repeatedly explained 
 that Edwards and Haime regarded: F. gothlandica as an essentially Silurian species; and 
 the corresponding Devonian form was separated by them under the name of F. Goldfussi. 
 The latter is stated by its authors to be distinguished from the former by its larger 
 corallites and more closely set mural pores. The size of the tubes (13 lines), however, is 
 frequently exceeded by typical Upper Silurian examples of F. gothlandica, notwith- 
 standing their more commonly smaller size. Under any circumstances, the size of the 
 eorallites merely cannot be regarded as a character of the smallest specific value, while 
 the mural pores exhibit an at least equal variability. Upon the whole, therefore, 
 F. Goldfussi, Hdw. and H., cannot be satisfactorily separated from F. gotllandica, 
 except as a mere variety. 
 
 In the specimens here referred to, F. gothlandica, var. Goldfussi, the diameter 
 of the calices, as before stated, is about 14 lines, in extreme cases reaching as much 
 as 2¢ lines. In one example there are four tabule in the space of 2 lines vertical, 
 whilst in another specimen the same number are contained in a space a little exceeding 
 this. The examples collected by the late Mr. Daintree appear to be only portions of 
 colonies; but notwithstanding this, one of the specimens, a very fine one, measures 
 93 by 43 inches, forming a more or less elongated depressed parallelogram. This 
 form of F. gothlandica corresponds in a striking manner with that met with in the 
 Corniferous Limestone of North America, a careful comparison having been made with 
 colonies of the latter coral in the cabinet of one of us. 
 
 We now come to four specimens, and possibly a fifth, which are regarded as 
 referable to Favosites gothlandica proper, a8 understood by Messrs. Edwards and 
 Haime. They also bear a close resemblance to F. epidermata, Rominger, from the 
 Corniferous Limestone of North America, which is probably, after all, only another 
 variety of the widely spread and typical &. gothlandica. In the colonies in question the 
 calices are much smaller, scarcely ever exceeding 1 line in diameter, and frequently less, 
 whilst four tabule appear, on an average, to be comprised within the space of 13 lines 
 vertical. We say on an average, because we find, on the examination of a sufficiently 
 large number of specimens gathered from various quarters, and including those from 
 Australia, that there is every gradation between the two conditions in the size of the 
 corallites and disposition of the tabule. It is on these grounds, combined with the 
 variable disposition of the mural pores, that we propose to consider F. gothlandica in 
 the wide sense understood by Goldfuss, before its subdivision by Edwards and Haime. 
 
 In the fifth example, previously referred to as probably identical with the other 
 form, the septal spines are well developed. (Nicholson and Etheridge fil.) 
 
 Loc. Broken River, a tributary of the Clarke River (Lhe late R. Daintree, 
 Collection British Museum, and Geological Survey of Queensland). A small fragment 
 of Favosites, probably F. gothlandica, has been more recently obtained by Mr. Jack 
 from the above locality. 
 
 Genus—PACH YPORA, Lindstrém, 1873. 
 (Ofver. K. Akad. Foérhandl., 1873, p. 14.) 
 
 PACHYPORA MERIDIONALIS, Wich. and Eth. jfil., Pl. 2, figs. 10-15. 
 P. meridionalis, Nich. and Eth. fil., Ann. and Mag. Nat. Hist., 1879, iv., p. 280. 
 
 Sp. Char. Corallum ramose, of cylindrical branches, about 23 lines or 3 
 lines in diameter, dividing dichotomously at comparatively remote intervals. Corallites 
 not regularly polygonal, with very thick walls, the diameter of which increases 
 as the mouth is approached. Calices hardly at all oblique, about a third of a line, 
 or sometimes rather more, in diameter, oval, rounded, or irregular in shape, often 
 
52 
 
 opening into one another, surrounded by thick obtuse margins, which exhibit no traces 
 of the original polygonal wall of the corallite. Mural pores few, very large, and 
 irregularly placed. Tabule few and remote. (Micholson and Etheridge fil.) 
 
 Obs. This species is unquestionably very closely allied to Pachypora cervicornis, 
 De Blainy., of the European Devonian, and we have felt some hesitation in giving it a 
 distinct specific designation. Both belong to that section of Fuavosites in which the 
 walls are thickened by the secondary deposition of sclerenchyma in successive lamine, 
 the amount of this thickening being increased as the mouth is approached, and are 
 therefore referable to Lindstrém’s genus Pachypora. Both are alike in form and general 
 habits, and have singularly large, sparse, andirregular mural pores. After a comparison, 
 however, of the Australian specimens with examples from the Eifel, macroscopically 
 and microscopically, we have come to the conclusion that the former must, in the mean- 
 while, be regarded as specifically distinct, upon the following grounds :— 
 
 (a) Pachypora meridionalis (nobis), is, on the whole, a much smaller species 
 than P. cervicornis, De Blainv., the branches in the latter often reaching 
 8 or 10 lines in diameter. 
 
 (b) The corallites in P. cervicornis can always be shown, by thin sections, to 
 preserve their polygonal outline, in spite of the thickening to which they 
 are subjected ; in the axis of the branches they are regularly polygonal, 
 and even the thickened lips of the calices show more or less distinctly a 
 polygonal line placed at a little distance from the mouth of the tube, 
 which represents the original wall. On the other hand, in P. meridionalis *® 
 the polygonal form of the corallites is more or less completely obliterated ; 
 even in the axis of the branches the originally prismatic wall cannot be 
 detected, and the thickened lips of the calices are simply rounded and obtuse. 
 
 (ec) In P. cervicornis the calices are about half-a-line in diameter, rounded or 
 sub-polygonal, and only occasionally opening into one another. In P. 
 meridionalis, on the contrary, the calices are mostly only about a third of a 
 line in diameter (counting in, as before, the wall around them); their shape 
 is very irregular, and they open into one another so frequently, and to such 
 an extent, that they sometimes become almost vermiculate in character. 
 
 Upon the whole, therefore, the present species is sufficiently distinct from 
 P. cervicornis, De Blainv., to deserve a separate name, and we know of no other 
 adequately characterised species with which it is necessary to compare it in detail. We 
 may add that the differences between P. meridionalis and P. cervicornis, above alluded 
 to, are much more conspicuous if we take specimens of the form usually known by the 
 latter name in the Devonian Limestones of Devonshire, and figured as such by Milne- 
 Edwards and Haime.* (Nicholson and Etheridge jil.) 
 
 Loe. Fanning River, Burdekin Downs, and Arthur’s Creek, Burdekin Downs; 
 Regan’s, Northern Railway, thirty-one miles from Townsville. (R. L. Jack.) 
 
 * Genus—ALVEOLITES, Lamarck, 1801. 
 (Emend. Nicholson, 1879.) 
 
 Alveolites, Lamk., Syst. Anim, sans Vertéb., 1801. 
 5 Nicholson, Tabulate Corals Pal. Period, 1879, pp. 117, 375. 
 Billingsia, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1876, Pts. 1, 2, p. 75. 
 Cladopora, Rominger, Report Geol. Survey Michigan, 1876, iii., Pt. 2, p. 50. 
 Obs. The chaotic condition in which the genus Alveolites remained for many 
 years has been commented on, and the genus made the subject of research by Prof. 
 
 
 
 * Mon, Brit, Dev. Corals, Pl. xlviii., fig. 2, 
 
 = 
 
Se 
 
 53 
 
 H. A. Nicholson, and the Writer,* and later by the former alone. As now restricted it 
 contains Favositiform corals with thin-walled corallites opening obliquely on the surface 
 by sub-triangular or semi-lunar calices. The septa are either obsolete or in the form of 
 longitudinal rows of spinules. It has been already pointed out by Mr. A. H. Foord and 
 the Writer + that the species upon which De Koninck’s genus Billingsia was founded is 
 a true Alveolites, and it follows, therefore, that Billingsia must now be considered a 
 synonym of the latter. Previous to this determination, Prof. H. A. Nicholson had 
 remarked,t “It seems hardly possible, with our present knowledge, to arrive at any 
 certain conclusions as to its true systematic position” (¢.e., of Billingsia). 
 
 Cladopora, Hall, as defined by Réminger,§ does not appear to differ essentially from 
 Alveolites. The corallites are said to be usually devoid of tabule, but Rominger 
 observes—‘ Their occasional development is proved by many actual observations.” 
 
 Under this name there have been deseribed from the Paleozoic rocks of Australia 
 the following species :—The Upper Silurian Series of Burrowang has yielded to the 
 researches of Prof. De Koninck,|| Alveolites repens, Fougt., and A. rapa, De Kon. The 
 so-called Lower Devonian rocks of the same Colony have yielded Alveolites subequalis, 
 Edw. and H., and A. obscurus, De Kon. The Queensland Alveolites in no way correspond 
 to any of these; indeed, the two new species described by Prof. De Koninck appear to 
 be very unsatisfactorily established, and nothing is known of their microscopic structure. 
 
 In addition to the foregoing, Prof. H. A. Nicholson and the Writer described two 
 imperfectly known species in 1879. 
 
 ALVEOLITES ALVEOLARIS, De Koninck, sp., Pl. 2, figs. 1-8a. 
 
 Billingsia alveolaris, De Kon., Foss. Pal. Nouv.-Galles du Sud, 1876, Pts. 1-2, p. 75, t. 2, f. 4 a, 0. 
 Alveolites alveolaris, Eth. fil. and Foord, Ann. and Mag. Nat. Hist., 1884, xiv., p. 176, t. 6, f. 1-le. 
 
 Sp. Char. Corallum massive and apparently lobate. Corallites minute (about 
 
 two in the space of a millim.), closely contiguous, of considerable length and their walls 
 
 somewhat thick ; the apertures of the calices present an irregularly lunate form, and in 
 some of them a single tooth-like septum may be detected. Tabule well developed, 
 horizontal, or a little curved and tolerably numerous. Mural pores large, in a single 
 series placed at pretty regular intervals of about half a millimeter apart. 
 
 Obs. The highly crystalline condition of the specimens rendered their determi- 
 nation very difficult. They occur in the shape of weathered masses in which some parts, 
 harder than the rest, stand out in relief and exhibit well the structures described 
 above. One of the specimens has the surface studded with small conical elevations, 
 about 1 centimeter apart, measured from their summits. The significance of these is 
 not apparent, and their occurrence is not known in any species of Alveolites. Of the 
 two species of Alveolites recorded from Australian Devonian rocks, only one (A. 
 subequalis, Ed. and H.) need be compared with the present form, and the much smaller 
 corallites of the latter afford sufficient grounds for their separation. 
 
 In his “ Paleozoic Fossils of New South Wales,’ Prof. L. G. De Koninck 
 instituted a genus under the name of Billingsia, for a Devonian coral from the 
 neighbourhood of Yass, which the author describes as apparently devoid of tabule 
 (‘‘ Les planchers semblent faire defaut’) and as possessing lateral openings in the walls 
 of the corallites resembling those of Syringopora. M. De Koninck appears to have 
 
 * Journ. Linn. Soc. (Zool.), xiii., p. 353. 
 
 + Ann. and Mag. Nat. Hist., 1884, xiv., p. 176. 
 
 + Tabulate Corals Pal. Period, 1879, p. 186. 
 
 § Report Geol. Survey Michigan, 1876, iii., Pt. 2, p. 50. 
 
 || Foss, Pal. Nouy.-Galles du Sud, 1876, Pt. 1, pp. 17, 18, 19. 
 
54 
 
 entirely misunderstood the structure of this coral. The figures given by that Author 
 accord remarkably well with our form; and although he states in his description that 
 tabule are wanting, they appear to be shown clearly enough in Fig. 4 of his work, as 
 cited. Assuming, then, that Billingsia alveolaris is identical with the Queensland 
 specimens, it is impossible to accept De Koninck’s suggestion that the present species is 
 transitional between Aulopora and Syringopora. 
 
 Loc. Regan’s, Northern Railway, thirty-one miles from Townsville. (2. L. Jack.) 
 
 ALVEOLITES ALVEOLARIS, var. QUEENSLANDENSIS, Lith. fil. and Foord, Pl. 2, figs. 4-6. 
 Alveolites alveolaris, var. queenslandensis, Eth. fil. and Foord, Ann. and Mag. Nat. Hist., 1884, 
 Den dig tanvivged eects 
 
 Obs. This form differs from that described above, chiefly in the size of the 
 corallites, which are considerably larger than those of A. alveolaris. It also appears to 
 be branching and lobulate, and occurs in large weathered and rounded fragments, one of 
 which measures about 12 centimeters in its greatest length, aud about 6 centimeters in 
 thickness, but the specimen must have been considerably larger when perfect. Scarcely 
 any of its surface remains, and microscopic sections do not yield very satisfactory results 
 on account of the extensive mineral alteration that the fossils have undergone. 
 
 In their longer diameter the corallites measure about two-thirds of a millimeter, 
 in their shorter about one-third or even less. The tabule are somewhat numerous, 
 horizontal or oblique, and sometimes curved, and in some places they anastomose. 
 The mural pores are large and apparently numerous. 
 
 Loc. Regan’s, Northern Railway, thirty-one miles from Townsville. (2. L. Jack.) 
 
 ALVEOLITES ROBUSTUS, Rominger, Pl. 1, figs. 13, 14. 
 Cladopora robusta, Rominger, Report Geol. Survey Michigan, 1876, iii., Pt. 2, p. 55, t. 22, f. 1, 2. 
 
 Obs. A ramose species, with affinities to Pachypora, and possibly really referable 
 to this latter genus. The surface characters are much destroyed by weathering, and as 
 its internal structure shows nothing but mural pores and tabule, with no special 
 features of interest, little further can be said about it. The coral may at once be 
 distinguished from Pachypora meridionalis by its very oblique tubes and calices. 
 
 The largest of the specimens hitherto examined (by no means a perfect one) is 
 33 inches in length. The distance between two points of bifurcation or dichotomiza- 
 tion of the branches is 1 inch 3 lines. 
 
 This species is very like <Alveolites (Cladopora) robustus, Roém., and so closely 
 resembles his smaller figure of that form that one is induced to refer it to the latter, 
 even without an actual comparison of specimens. The Queensland examples possess 
 the same habit of growth as those from Michigan, and the calices correspond in size 
 with the figures indicated. Alveolites robustus, Rém., is met with both in the Cornifer- 
 ous and Hamilton Groups (Lower and Middle Devonian) of North America. 
 
 Loc. Arthur’s Creek, Burdekin Downs. (R. L. Jack.) 
 
 ALVEOLITES, sp. ind., Pl. 1, figs. 15-17. 
 Alveolites, sp. ind., Nicholson and Eth. fil., Ann. and Mag. Nat. Hist., 1879, iv., p. 222. 
 
 Obs. An expanded, lobate, or palmate form, which, in the present unsatisfactory 
 and chaotic state of Alveolites, is very difficult to determine, although, specifically 
 speaking, we do not know anything precisely like it. Sections show that the corallites 
 were thin-walled and irregular, with mural pores and plenty of tabule. With the 
 meagre material before us, it would be only unnecessarily increasing nomenclature to 
 bestow a name. (Nicholson and Etheridge fil.) ' 
 
 Loc, Arthur’s Creek, Burdekin Downs. (R. ZL. Jack.) 
 

 
 55 
 Genus—AMPLEXOPORA, Ulrich, 1882. 
 
 (Journ, Cincinnati Soc. Nat. Hist., v., p. 154.) 
 Amprexopora? Koninexi, Etheridge fil. and Foord, Pl. 2, figs. 7-9a. 
 Amplexopora Koninckii, Eth. fil. and Foord, Ann. and Mag. Nat. Hist., 1884, xiv., p. 178, t. 6, f. 3 a-c. 
 
 Sp. Char. Corallum massive. Calices. polygonal in outline, with the angles 
 rounded, minute and variable in size, somewhat thin-walled; from three to four occupy 
 the space of 1 millimeter. Spiniform corallites placed at the angles of junction of 
 many of the cell apertures. Tabule remarkably regular, horizontal, from 1 to 2 tube 
 diameters apart. 
 
 Obs. The present species, like the others from the same locality, has undergone 
 a good deal of alteration by weathering and crystallisation, so as to obscure, in a measure, 
 the structure of the organism. ‘The in-filling of the coral is calcite of fibrous structure 
 (Arragonite?), the fibres cutting the walls of the corallites, as well as crossing the 
 visceral cavities. 
 
 The first impression gained on examining thin sections of this coral was that it 
 might be a Chetetes ; but the presence of the spiniform corallites (provided, of course, 
 these structures have been correctly interpreted), sets this question at rest. 
 
 Loc. Regan’s, Northern Railway, thirty-one miles from Townsville. (2.L. Jack.) 
 
 Genus—TRACHYPORA, Edw. and Haime, 1851. 
 (Polyp. Foss. Terr. Pal., p. 305.) 
 
 TRACHYPORA, sp. ind. 
 Trachypora, sp. ind., Nicholson and Eth. fil., Ann. and Mag. Nat. Hist., 1879, iv., p. 281. 
 
 Obs. A single and badly preserved example has occurred in the Arthur’s Creek 
 Limestone, which, although sufficiently good for generic identification, is in too ill- 
 preserved a condition to warrant us in attaching to it a specific description and name. 
 
 The specimen is seated on the weathered surface of a piece of limestone, and 
 exhibits the vermiculate surface and non-septate calices characteristic of Trachypora. 
 
 Loc. Arthur’s Creek, Burdekin Downs. (2. LZ. Jack.) 
 
 Genus—STRIATOPOCRA, Hall, 1852. 
 (Pal. New York, ii., p. 156.) 
 STRIATOPORA ? UNISEPTATA, sp. nov., Pl. 37, figs. 1, 2. 
 
 Sp. Char. Corallum small, dendroid, composed of bifurcating cylindrical stems. 
 Corallites thick-walled, the calices arranged in vertical rows separated by thickened 
 sclerenchyma, with oval, oblique, cup-shaped apertures, of more or less equal dimen- 
 sions; the orifices below are circular and contracted, the distal wall invariably bearing 
 a single septal ridge. Pores small, not numerous, scattered. Tabule ? 
 
 Obs. In some respects this little coral resembles Striatopora, as in the arrange- 
 ment of the cells, and the form of their orifices. On the other hand, it differs widely 
 in the separation of the former by the interstitial ceenenchyma, and in the presence of a 
 single septum only; in fact, I much question the propriety of retaining it in this 
 genus. The single septum is a very constant character in each calice, as a vertical 
 ridge on the distal, on hinder wall, apparently descending far into the former. 
 
 I have not observed any definite trace of tabule, the material being too limited 
 in quantity to permit of the preparation of microscopic sections. In the weathered 
 portion of the specimen these delicate organs have been removed. Judging from a 
 natural transverse section the corallites seem to have had well-developed walls in the 
 centre of the corallum. and to pass outwards by a very gentle and gradual curve, 
 
56 
 
 The poriferous nature of the walls clearly indicates this as a member of the 
 Favositide, although it is quite possible that it may be referable to a genus other than 
 Striatopora. 
 
 A similar septal tooth occurs in a French Devonian fossil, Zrachypora marmorea, 
 Gosselet.* 
 
 Loc. Fanning River. (R. L. Jack.) 
 
 Genus—ROMINGERIA, Nicholson, 1879. 
 (Tabulate Corals Pal. Period, p. 114.) 
 RoMINGERIA ? Foornt, sp. nov., Pl. 1, fig. 18. 
 
 Sp. Char. Corallum ramose. Corallites small, tubular, their outlines faintly 
 indicated on the surface of the branches. Calices oval or circular, exsert or slightly 
 disjunct, sub-opposite, sometimes contiguous, and almost touching one another. 
 
 Obs. It is quite an open question whether this coral should be placed in 
 Romingeria or Vermipora, but probably in one or the other, notwithstanding its ramose 
 character. Although the surface is much weathered, the tubular outline of the corallites 
 is dimly portrayed on the branches, and this would to some extent ally it to the still 
 more divided-up corallum of one or other of the above genera. At the broken distal 
 end of the specimen the tubular state of the corallites is quite apparent. 
 
 The surface is too much weathered to show the annulations described by Prof. 
 Nicholson in his genus, even if they existed, and, from the same cause in all probability, 
 septa are not visible. 
 
 Named in honour of Mr. A. H. Foord, late of the Geological Survey of Canada, 
 with whom the Writer has been engaged in paleontological investigation. 
 
 Loc. Reid Gap, thirty-one miles from Townsville. (&. ZL. Jack.) 
 
 Genus—C@NITES, Hichwald, 1829. 
 (Zoologia Spec., I., p. 179.) 
 
 Obs. Cenites is represented by a few ramose or frondescent specimens, with the 
 general aspect of Cenites expansus, De Koninck (PI. 2, figs. 18 and 19), the mouths of the 
 calices corresponding in size and shape, but there are usually present three instead of two 
 septal teeth. The specimens are not sufficiently well preserved for accurate determination. 
 
 Loc. Regan’s, Northern Railway. (R. L. Jack.) 
 
 Family—PORITIDZ. 
 
 Genus—ARAOPORA, Nicholson and Etheridge jil., 1879. 
 
 Arcopora, Nicholson and Eth. fil., Ann. and Mag. Nat. Hist., 1879, iv., p. 277. 
 PF Nicholson, Tabulate Corals Pal. Period, 1879, p. 105. 
 a Waagen and Wentzel, Paleontologia Indica, 1886, Ser. xiii., Pt. i., No. 6, p. 837, 
 
 Gen. Char. Corallum massive, resembling that of uvosites, of polygonal 
 corallites, which radiate outwards from an imaginary axis to open upon the upper 
 surface of the colony. Under surface covered with an epitheca (?). The corallites are 
 firmly united by their walls, which are extensively pierced by apertures, placing the 
 visceral tubes in direct communication. Septa trabecular, often irregularly divided or 
 anastomosing at their free ends. Tabule rudimentary, represented by occasional 
 horizontal trabecule. No columella nor ccenenchyma. (Wicholson and Etheridge fil.) 
 
 Obs. This genus was founded upon a single remarkable specimen belonging to 
 the Daintree Collection, from the Devonian deposits of Queensland, distinguished 
 specifically by the name of Arwopora australis. 
 
 
 
 * Ann. Soc. Géol. du Nord, 1877, iv., t. 3, f. 2a. 
 

 
 57 
 
 Since the description of Arwopora by Prof. H. A. Nicholson and the Writer 
 appeared, Messrs. Waagen and Wentzel have re-defined* the genus from material 
 obtained from the rich beds of the Salt Range in India, with the result that the 
 “characteristic of the genus must be changed to a certain extent in some points to fit 
 the Salt Range species.” Several points in their observations appear to call for remark. 
 In the first place Ar@opora is ascribed to Nicholson alone, as given in his “ Tabulate 
 Corals,’ published in 1879. Messrs. Waagen and Wentzel appear wholly to ignore the 
 heading which they quote from this work as given by Prof. Nicholson, viz., “ Argopora, 
 Nich. and Eth. jun., 1879.’’ Secondly, the above Authors appear to be unacquainted 
 with, or to have overlooked the description of Ar@opora given by Prof. Nicholson and 
 the present Writer,} which, as a matter of fact, was published before the “ Tabulate 
 Corals,” and is the original and first published description of the genus. Had this not 
 been so we should have referred, in preparing our joint memoir, to Prof. Nicholson’s 
 work. Messrs. Waagen and Wentzel, in the third place, state—“ No mention is made by 
 Nicholson of the spongy condition of the walls of the corallites.” Not in so many 
 words, perhaps, but in the expression “ porous condition of the walls,’ used both in the 
 “Tabulate Corals” and in our joint Memoir, far more is implied than that the walls are 
 merely pierced by mural pores. In addition, the figures gave an excellent idea of the 
 spongy nature of the walls. Lastly, the Authors say— Another point which has to be 
 rectified is the condition of the tabule. They are well developed and quite distinct, 
 not rudimentary, in the Indian species.” What the tabule may be in the latter it would 
 be presumptuous for us to say, in the absence of specimens; but although they may be 
 well marked in the Indian species that does not prove them to be anything else than 
 rudimentary in the Australian form. It is quite possible that amplification of the 
 characters of our genus may be required—as is usually the case in the first descriptions 
 of obscure fossils—but this hardly approaches the authoritative “ rectification ” 
 imagined by Messrs. Waagen and Wentzel. 
 
 Type. Areéopora australis, N. and E. fil. 
 
 ARRHOPORA AUSTRALIS, Nich. and Eth. jfil., Pl. 3, figs. 6-9. 
 
 Arcopora australis, Nicholson and Eth. fil., Ann. and Mag, Nat. Hist., 1879, iv., p. 278, p. 279, f. 3 a, b. 
 An a Nicholson, Tabulate Corals Pal. Period, 1879, p. 167, f. 24 a, b. 
 
 Sp. Char. Corallum massive, pyriform, of considerable size, composed of poly- 
 gonal or prismatic corallites which radiate outwards from an imaginary axis to open on 
 the upper surface of the colony. Average diameter of the corallites from two-thirds to 
 three-fourths of a line, no very small tubes being intercalated amongst those of 
 ordinary dimensions. Walls amalgamated, irregularly cribriform. Septa variable in 
 number, spiniform, or irregularly divided. Tabule rudimentary. (Wicholson and 
 Etheridge fil.) 
 
 Obs. The corallum of A. australis might at first sight be readily taken for that 
 of any of the larger and more massive species of Favosites (such as Ff. hemisphericus, 
 Yand. and Shum.), though even to the naked eye the absence of distinct tabule and 
 the cribriform or porous condition of the walls are striking features. Our only 
 specimen is not perfect, and is not only completely silicified, but is thoroughly infiltrated 
 with silica tinged with oxide of iron. Its height is rather more than 38 inches, and 
 its greatest width something over 4 inches. Its form is pyriform, the narrow base 
 having evidently been attached to some foreign body, while the under surface was 
 almost certainly covered by an epitheca, of which no traces now remain. The calices 
 
 
 
 * Paleontologia Indica, Ser. xiii., Pt. i., No. 6, Coelenterata, p, 837. 
 + Ann. and Mag. Nat. Hist., 1879, Vol. iv., p. 277. 
 
58 
 
 must have opened over the whole of the upper surface, but none of them are preserved 
 in the specimen now before us. The corallites radiate with a graduated divergence from 
 the imaginary axis of the colony; and their form is regularly prismatic or polygonal, as 
 in Favosites. This character, however, is much more perceptible by the eye, or when 
 the surface is examined with a lens, than it is when thin sections are investigated under 
 the microscope, as it is to some extent marked in the latter case by the broken and 
 cribriform structure of the walls. Thin sections (Pl. 3, figs. 7 and 9), whether trans- 
 verse or vertical, show that the walls of the tubes are extensively porous and cribriform, 
 being pierced by numerous apertures, which place the visceral chambers in direct com- 
 munication. Transverse sections also serve admirably to show the character of the 
 irregular trabecular septa, some of which are simply spiniform, while others divide 
 towards their inner extremities, or even unite with their neighbours by their free ends. 
 Vertical sections show that the septa are upon the whole placed in longitudinal rows, 
 and they exhibit occasionally horizontal trabecule (PI. 3, fig. 9), which may be regarded 
 as of the nature of rudimentary tabule. 
 
 From a consideration of the above characters it cannot be doubted that we have 
 to deal, in Areopora, with a genuine ‘ Perforate” Coral, which, however, is closely 
 related to the Favositidw, and may be best placed in this family rather than in any of 
 the more regular groups of the Perforata. By the characters of its walls and septa the 
 genus presents certain alliances with the Poritide; but its general form and aspect are 
 those of a Fuvosites ; and the presence of rudimentary tabule would further confirm 
 the view here taken. Among the genera of the Favositide, its nearest ally is to be 
 found in the Lower Silurian genus Columnopora, Nich., which it nearly resembles in 
 form and habit. It is distinguished from the latter, however, by the less regularly 
 perforate character of its walls, by the rudimentary condition of its tabule, and by the 
 irregularly dividing and trabecular septa. Weare unable to institute any comparison 
 between dr@opora and the Cretaceous genus Koninckia, EH. and H., but the septa of the 
 latter seem to be merely spiniform (six in number), and the tabule are said to be well 
 developed and complete. (Nicholson and Etheridge fil.) 
 
 Messrs. Waagen and Wentzel have removed Areéopora from the Favositide and 
 placed it in the Poritide. It is possible this step may be quite justifiable. 
 
 Loc. Burdekin River. (Lhe late Rk. Daintree; Colln. Brit. Mus.) 
 
 Order—RUGOSA. 
 Family—CYSTIPHYLLID. 
 
 Genus—CYSTIPHYLLUM, Lonsdale, 1839. 
 (Murchison’s Silurian System, p. 691.) 
 CYsTIPHYLLUM AMERICANUM, Edw. and Haime, var. AUSTRALE, var. nov., Pl. 8, 
 figs. 18, 14. 
 
 Obs. Up to the present time we are not acquainted with any published species 
 of Oystiphyllum from Australian Devonian rocks, but a species has been met with in the 
 Silurian beds of Burrowang, New South Wales. The coral reefs at Regan’s on the 
 Northern Railway, however, have yielded several examples of a very elongate species, 
 with a general resemblance to the British Devonian C. vesiculosum, Goldfuss, but the 
 vesicles of the corallum are much too large. On the whole the corals appear to come 
 nearest to the American form ©. americanum, and for all practical purposes may be 
 regarded as a variety of it. In only one example has any tendency to a funnel or cone 
 shaped outline been observed, such as occurs in C. senecalense, Billings,* but not 
 
 
 
 
 
 * Canadian Journal, 1859, p. 137, 
 

 
 59 
 
 sufficiently so to render it in any way allied to the latter. The length of the corallum 
 would also indicate C. conifollis, Hall,* as an ally, but no indication of the epithecal 
 swellings of the latter occur in our form. 
 
 Loe. Regan’s, Northern Railway, thirty-one miles from Townsville. (2. L. Jack.) 
 
 Genus—CYATHOPHYLLUM, Goldfuss, 1826. 
 (Petrefacta Germanie, i., I Theil, p. 54.) 
 
 CYATHOPHYLLUM, sp. ind., Pl. 3, figs. 11, 12. 
 
 Obs. A few turbinate corals are associated with the more numerous specimens 
 of the last species, which appear referable to the genus Oyathophyllum. The small 
 amount of material, however, for investigation, and the large number of species of this 
 genus at present known, render the task of identification difficult. 
 
 The complete corallum is unknown, but it was short and conical, or turbinate, with 
 numerous septa—at least fifty-fourin number. They are long and almost straight, every 
 alternate one extending to the centre of the ealice, the others not beyond the outer 
 vesicular zone; the longer or primary septa are more or less confusedly intermingled or 
 slightly twisted at the centre, giving rise toa loosely vesicular structure. The interseptal 
 loculi are filled with large vesicles, forming an outer vesicular zone, extending inwards 
 for quite half the width of the corallum. The fossula is apparently absent. 
 
 This species is evidently of the same type of growth as C. virgatum, Hinde,t and 
 may possibly be it, as the number of septa closely correspond. 
 
 Lec. Regan’s, Northern Railway. (&. L. Jack.) 
 
 In Leichhardt’s “ Journal of an Overland Expedition in Australia,”’{ the Rey. 
 W. B. Clarke described a coral from the Burdekin Limestone § as Cyathophyllum Leich- 
 hardti. His description is here appended, but unfortunately little or nothing can be 
 made of it from a systematic point of view. The name might be deleted with 
 advantage to Australian Paleontology. The description is as follows :— 
 
 “The most conspicuous fossil is a coral which appears to belong to the family of 
 Cyathophyllide. The genus is perhaps new, but this the want of specimens with which 
 to compare it does not allow me the means of verifying. It may, however, be classed 
 provisionally as Cyathophyllum, to which in many respects it bears a great resemblance. 
 
 “Cells concavely cylindrical, not dichotomous (thus distinguished from Caryo- 
 phyllia) grouped but separate, laterally if at all proliferous. Corallum beautifully 
 stellular, formed by 30-35 slightly spirally curving or regular radiating lamellw, which 
 meet in a central point or overlap on a latitudinal axial line, and are divided by 
 rectangular or outwardly convex and upwardly oblique dissepiments, which become 
 occasionally indistinct or obsolete near the centre, thus not assuming the usual charac- 
 teristic of Cyathophyllum but rather one of Strombodes. 
 
 “Surface longitudinally striated, the cellular structure being hidden in calcareous 
 spar, the striz formed by the coalescing lamellx, which, at the extremities, seem to be 
 occasionally denticulated owing to the matrix interrupting their passage to the edge. 
 This resembles what takes place in some Astreeide. 
 
 ‘The interior has more the features of Acervularia than Cyathophyllum, but 
 there are patches of broken transverse septa in the rock which exhibit the features of 
 the latter.” 
 
 
 
 * Pal. N. York, Illustrations of Devonian Fossils, 1876, t. 3, f. 3-9. 
 
 + Geol. Mag., 1890, vii. (3), p. 194, t. 8, f. La, 6. 
 
 t Journal of an Overland Expedition in Australia from Moreton Bay to Port Essington during the 
 years 1844-45 (8vo., London, 1847), p. 212. 
 
 § “ About Lat. 19° 58’ 11”S.” [Probably Burdekin Downs. R&.L.J.] 
 
60 
 
 Family—ZAPHRENTID. 
 
 Genus—AM PLEXUS, J. Sowerby, 1814. 
 (Min. Con., i., No. 18, p. 165.) 
 
 AMPLEXUS, sp. ind., Pl. 87, figs. 15, 16. 
 
 Obs. <A single fragment of an Amplexus from the Broken River Limestone has 
 some relation to 4. Selwyni, De Koninck, but it is very much smaller and possesses only 
 half the number of septa. There is no trace of a septal fossula at all, and in all proba- 
 bility the epitheca was very thin. There are about thirty septa, and the coste are 
 regular and very apparent, whilst the central tabular space is large for the size of the 
 corallum. Although the specimen is only a fragment, the corallum was evidently 
 cylindrical and somewhat curved. 
 
 Loc. Broken River, a tributary of the Clarke River. (2. L. Jack.) 
 
 Genus—CAMPOPHYLILUM, Edwards and Haime, 1850. 
 (Mon. Brit. Foss. Corals, Pt. 1, p. xviii.) 
 
 CAMPOPHYLLUM GREGORII, sp. nov., Pl. 3, figs. 15-18. 
 
 Sp. Char. Corallum long, either straight or gently curved, and sometimes 
 slightly twisted. Epitheca apparently thin, and with indistinct growth accretions. Septa 
 numerous, sixty at least, gradually tapering at the extremities; secondary septa less than 
 half the length of the primary, and much more slender. Vesicular tissue forming a 
 zone having a width about equal to the length of the secondary septa, the vesicles small 
 and close together. Septal fossula large, containing one primary septum (or some- 
 times two?) Central tabulate area conspicuous, almost equal in breadth to the length 
 of the primary septa. Tabule horizontal, or sometimes slightly oblique and very close 
 to one another, in places almost touching. 
 
 Obs. The genus Campophyllum has not been extensively recognised as Devonian, 
 but investigation will probably prove it to have flourished at that period to a greater 
 extent than has been supposed. Prof. L. G. De Koninck has recorded the occurrence 
 of Campophyllum flecuosum, Ed. and H., in the Lower Devonian Series of Quadong, 
 N.S. Wales, but I believe this is the only species yet recognised in Australia. The 
 present coral is quite distinct from the latter, and I feel much pleasure in associating 
 with it the name of the Hon. A. C. Gregory, who has for so many years been connected 
 with Australian science and exploration. 
 
 Loc. Regan’s, Benwell’s, and Philp’s, Northern Railway. (&. L. Jack.) 
 
 Order—ALCYONARIA. 
 Family—HELIOLITIDZ. 
 
 Genus—HELIOLITES, Dana, 1846. 
 (Zoophytes, Wilkes U. 8. Expl. Exped., p, 541.) 
 
 Obs. The Silurian and Devonian rocks of one or other of the Australian 
 Colonies have yielded six species of this genus, so far as present researches have gone, 
 and to these we have to add a seventh and eighth. 
 
 Heliolites interstinctus, Linn., has been met with, according to Prof. McCoy,* 
 in the Upper Silurian Limestone of Waratah Bay, Victoria. The researches of Prof. 
 De Koninck have shown the existence of H. megastoma, McCoy, and H. Murchisoni, in 
 
 
 
 
 
 
 
 * As Palcopora, in Progress Report for 1876, No, iv., Geol. Survey Vict., by T. Couchman, pp. 156, 
 158 (Melbourne, 8vo., 1877). 
 
~~ 2 e 
 
 61 
 
 the Upper Silurian rocks (probably Ludlow or Wenlock) of New South Wales, at 
 Burrowang,* whilst the supposed Devonian of the same colony has yielded ZH. porosa, 
 Goldf.+ The same species has been shown by Prof. Nicholson and the Writer to occur 
 plentifully in the Devonian Limestones of North Queensland, accompanied by three 
 other and interesting forms—viz., Heliolites Daintreei, H. plasmoporoides, and an indi- 
 cated species which is now named Heliolites Nicholsoni. The most aberrant species 
 of the genus is H. plasmoporoides, Eth. fil. and Nich., which nearly approaches the genus 
 Plasmopora, by its comparatively irregular and few interstitial tubes. 
 
 HeEtiorites porosa, Goldfuss, Pl. 1, fig. 6. 
 
 Astra porosa, Goldfuss, Petrefacta Germaniz, 1826, i., p. 61, t. 21, f. 7. 
 
 Heliolites porosa, M.-Edwards and Haime, Polyp. Foss. Terr. Pal., 1851, p. 218. 
 Be of M.-Edwards and Haime, Mon. Brit. Foss. Corals, 1853, Pt. 4, p. 212, t. 47, f. 1 a-f. 
 rE », De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1876, Pts. 1, 2, p. 81. 
 f as Nicholson and Eth. fil., Ann. and Mag. Nat. Hist., 1879, iv., p. 223. 
 
 Obs. Under this name we have assembled from localities in North Queensland 
 a series of specimens varying more or less slightly in their characters amongst them- 
 selves, but which we think are all referable to Heliolites porosa, Goldf. The composite 
 corallum in these corals is massive, with a flat under surface or base, having few and 
 faintly marked concentric ridges. The calices in all the specimens are circular, pretty 
 equally developed in the same individual, and separated by unequal interspaces occupied 
 by ccenenchymal tubes {; each calice varies from 4 to 3 line in diameter. The tubes 
 of the coenenchyma are rather small and polygonal, and constitute somewhat large 
 interspaces between the corallites. The septa are only visible here and there. 
 
 Upon comparing a series of specimens of A. porosa from German and British 
 Devonian rocks, we find that considerable variation takes place—1st, in the diameter of 
 the corallites themselves; 2nd, in the size of the coonenchymal tubuli; 3rd, in the 
 amount of intercalicular space occupied by the latter; and 4th, in the length of the 
 septa. These variations are, indeed, shown in the figures given by MM. Mailne- 
 Edwards and J. Haime. So far as we are able to judge, the Queensland examples 
 appear to occupy a median place in the above scale; the diameter of the corallites and 
 ccenenchymal tubuli is greater than in some European examples and less than in others, 
 On the whole the interspaces occupied by the tubuli are perhaps greater in the Queens- 
 land examples. 
 
 In vertical sections we can distinguish with ease the tabule, as described by 
 Edwards and Haime, horizontal, but sometimes oblique. These authors describe the 
 ccenenchymal tubuli as “ nearly regularly hexagonal.’’ Certainly this is the case with 
 some of the tubes on various parts of the Queensland specimens; but we find by far 
 the commoner form is the polygonal. 
 
 Loc. Broken River, a tributary of the Clarke River (Zhe late R. Daintree) ; 
 Fanning River, Burdekin Downs; Arthur’s Creek, Burdekin Downs (&. L. Jack). 
 
 Hetiorires Datntreer, Etheridge fil. and Nicholson, Pl. 1, figs. 7, 8. 
 Heliolites Duintreei, Nicholson and Eth, fil., Ann, and Mag, Nat. Hist., 1879, iv., p. 224, t. 14, f. 3a, 0. 
 Sp. Char. Corallum compound, discoid or flattened; upper surface a little 
 convex; under surface more or less flattened, concentrically wrinkled round the edges. 
 
 
 
 * Foss. Pal. Nouv.-Galles du Sud, 1876, Pt. i., pp. 24, 25. 
 
 + Ibid. p. 81. , 
 
 +In this and in the following descriptions of species of Heliolites the terms ‘‘ coenenchyma” and 
 ** conenchymal tubes” are used simply in accordance with previous custom, and for the sake of convenience. 
 There is, of course, no true ‘‘ccenenchyma” in Heliolites and its allies, and the so-called ** ccenenchymal 
 tubes” are really a specialised series of small corallites, 
 
62 
 
 Calices large, equal in size, with a diameter of 3-line, or at times almost 1 line, closely 
 set; calicular edge deeply scalloped. Septa numerous and well marked, certainly 
 fourteen and sometimes more, unequal in size. Cconenchyma composed of large and 
 well-developed tubes separating the corallites by irregular interspaces, often of small 
 extent. A specimen measures 3} by nearly 4 inches. (Micholson and Etheridge fil.) 
 
 Obs. .H. Daintreei may be distinguished by the size and contiguity of the large 
 corallites, with their strongly scalloped margins. The ccenenchymal tubuli are irregu- 
 larly developed, for between neighbouring calices we occasionally see only one row of 
 tubes, but more commonly the number is increased to two. The latter number varies 
 up to three or four, beyond which we have not observed them to be increased. 
 
 In the contiguity of its calices and frequent diminution of the tubuli, H. Dain- 
 treei resembles H. megastoma, McCoy, of the British Silurian rocks, but is at once 
 distinguished by the prominent scalloped edges of the calices, and the flat or little- 
 convex form of the corallum. 
 
 In the contiguity of the corallites one to the other there is a good deal of 
 resemblance between H. Daintreei and H. pyriformis, Lonsdale, as figured by Hall 
 from American specimens, but the other characters are quite dissimilar. (Wicholson 
 and Etheridge jil.) 
 
 Loc. Broken River, a tributary of the Clarke River. (The late R. Daintree.) 
 
 HIELIOLITES PLASMOPOROIDES, Ltheridge fil. and Nicholson, Pl. 1, figs. 9-11. 
 Heliolites plasmoporoides, Nicholson and Eth. fil., Ann. and Mag. Nat. Hist., 1879, iv., p. 25, t. 14, f. 2 a, 0. 
 . %~ Nicholson, Tabulate Corals Pal. Period, 1879, p. 245. 
 
 Sp. Char. Corallum irregularly ovate; upper surface convex. Calices circular, 
 with a thin thread-like margin, average diameter 1} line, contiguous, but separated from 
 one another by small interspaces of ccenenchymal tubuli. The latter are large and of 
 very irregular form; some are elongate with one axis much longer than the other, others 
 are polygonal; and, again, others are without definite outline. Between contiguous 
 corallites there is usually but one row of large oblong interstitial tubes, reaching from 
 calice to calice; or, where the corallites become a little separated from one another, 
 these may be increased in number. Septa almost obsolete, thread-like. A specimen 
 measures 5 inches by 4. (Micholson and Etheridge fil.) 
 
 Obs. The form and arrangement of the ceenenchymal tubuli render the present 
 species a very interesting one. If horizontal sections in the mass are examined only 
 with the naked eye or ordinary lens, the species will be pronounced a Plasmopora ; and 
 this it at first appeared to us to be. It has all the general appearance of this genus, 
 especially in the fact that there is often but a single row of oblong interstitial tubes 
 between every two corallites. In such sections the walls of these tubes have quite the 
 appearance of thread-like coste radiating from corallite to corallite, or bifurcating at 
 various angles where their number is increased between the corallites, as in Plasmopora. 
 When, however, vertical microscopic sections are examined, the true affinities of this 
 peculiar coral at once become apparent. In the first place, the arched and vesicular 
 tabule of Plasmopora are wanting, and we find in their place the straight horizontal 
 diaphragms of Heliolites. Secondly, in similar sections the interstitial or cenenchymal 
 structure is found not to consist of vertical canaliculi formed by the irregularly 
 developed walls of the tubuli, and subdivided by horizontal or convex dissepiments into 
 irregularly formed cells as in Plasmopora, but of a series of small, regular, and well- 
 developed cells formed by the intersection of the vertical tubuli and their horizontal 
 tabule, which are usually placed on the same level and correspond with one another, 
 precisely as seen in vertical sections of Heliolites megastoma, McCoy. 
 
————_ ~~ 
 
 
 
 63 
 
 So far as our investigations enable us to form an opinion, H. plasmoporoides is 
 most nearly allied to H. megastoma, McCoy; indeed, in the figure of this species given 
 by Edwards and Haime we notice the one-celled disposition of coenenchyma in places 
 similar to that seen in the present species. The latter, however, is clearly distinguished 
 from H. megastoma. (Nicholson and Etheridge fil.) 
 
 Loc. Broken River, a tributary of the Clarke River. (Zhe late R. Daintree.) 
 
 Hettorires Nicworsonl, sp. nov., Pl. 1, fig. 12. 
 Heliolites, sp. ind., Nicholson and Eth. fil., Ann. and Mag. Nat, Hist., 1874, iv., p. 225. 
 
 Sp. Char. Corailum in the form of rounded or sub-lobate masses of small 
 dimensions. Corallites circular, separated from one another by intervals of coonenchyma 
 varying from 2 to 2} millimetres in diameter. Calices very small, about $-mm. across, 
 with very thin and thread-like margins ; septa delicate and short; tabule moderately 
 close and nearly horizontal. Ccenenchymal tubuli exceedingly delicate and small, 
 almost microscopic, hexagonal or polygonal; tabule quite horizontal and moderately 
 close. 
 
 Obs. A third and small species of Heliolites is represented by several examples 
 nestling in the middle of a large block of Favosites. The calices and ccnenchymal 
 tubuli are very small, the latter so much so that the use of a lens is required for their 
 detection. 
 
 In a vertical section the structure is characteristically heliolitiform. In the 
 interspaces between the corallites, the small square cells making up the ccenenchyma 
 are quite apparent, but rather unequal in size. The tabule in the corallites are 
 moderately close and horizontal. 
 
 Traces of very small septa remaining in one or two of the corallites have been 
 observed, but their structure is so delicate and minute that their preservation is 
 surprising. It is very probable that this is an undescribed minute Heliolites, for which 
 the name of H. Nicholsoni is proposed. It appears to be smaller in general than any 
 of the commoner species of Heliolites, especially as regards the size of the coenenchymal 
 tubes. ; 
 
 Loc. Broken River, a tributary of the Clarke River. (Zhe late R. Daintree.) 
 
 Family—A ULOPORID. 
 
 Genus—AULOPORA, Goldfuss, 1826. 
 (Petrefacta Germaniz, i., I Theil, p. 82.) 
 
 AULOPORA REPENS (Knorr and Walch.), Edwards and Haime. 
 Aulopora serpens, Goldfuss, Petrefacta Germanie, 1826, I Theil, p. 82, t. 29, f. 1. 
 
 3 repens, Edwards and Haime, Polyp. Foss. Terr. Pal., 1851, p. 312. 
 
 Fe », Nicholson and’Eth. fil., Ann. and Mag. Nat. Hist., 1879, iv., p. 282. 
 
 A », Hinde, Geol. Mag., 1890, vii. (3), p. 199, t. 8, f. 5. 
 
 Obs. We have an example of this interesting coral creeping over the surface of 
 a specimen of Heliolites porosa. The weathering of the surface of the coral has 
 removed the epitheca and exposed wall of the Awlopora, and laid bare the interiors of 
 the ramifying or stolon-like corallites. (Micholson and Etheridge fil.) 
 
 The spaces enclosed by the union of the corallites are irregular in shape, some 
 polygonal, others elongated. The corallites either occur along the course of the 
 creeping network, or are thrown off asa small projection at each bifurcation. There is 
 no regularity in their disposition; at one point they succeed one another very rapidly 
 along the creeping tubes, and are much crowded; but on other portions they are 
 scattered and separated by much greater interspaces. On the edge of the corallum, 
 
64 
 
 where the reticulation becomes of a more open nature, the zigzag appearance given to 
 the corallites by frequent dichotomization becomes very apparent. There are no septa 
 visible in this example. (Nicholson and Etheridge Jil.) 
 
 Loc. Arthur’s Creek, Burdekin Downs. (R&R. L. Jack.) 
 
 AULOPORA, sp. ind. 
 
 Obs. The habit of growth of a second species from a different locality resembles 
 the Eifelian coral Awlopora spicata, Goldfuss.* Its general aspect is that of the genus 
 Vermipora, Hall, a likeness which is strengthened by the fact that Prof. H. A. 
 Nicholson} has suggested the reference of A. spicata to this genus. One specimen 
 appears to possess mural pores, a character which, if present, would assist in setting the 
 question at rest. 
 
 Another specimen from the same locality ramifies around a rugose coral, and is 
 surrounded by aStromatoporoid. Microscopic sections of this specimen display nothing 
 more than the ordinary auloporoid structure. It possesses the habit of Syringopora 
 auloporoides, De Kon.,t but is much smaller, and appears to be a true Awlopora. 
 
 . Loc. Regan’s and Philp’s, Northern Railway. (&. LZ. Jack.) 
 
 Sub-Kingdom—ECHINODERMATA. 
 Section—PELMATOZOA. 
 Class—CRINOIDEA. 
 Order—PALEOCRINOIDEA. 
 
 Of the Palxocrinoidea from Queensland localities, none have yet been brought 
 under my notice. I can only record that Mr. Jack reports that Encrinites are of 
 common occurrence in shales interstratified with the limestone beds of the Broken 
 River. Mr. Jack informs me that the Encrinites were unmistakable; but as he was 
 aware that their state of preservation would not permit of specific determination, he 
 did not, considering the difficulties of transit, bring away any specimens. 
 
 Sub-Kingdom—MOLLUSCA. 
 Class—BRACHIOPODA. 
 
 Order—TRETENTERATA. 
 Family—SPIRIFERID ZA. 
 
 Genus—SPIRIFERA, J. Sowerby, 1816. 
 (Min. Con., ii., p. 41.) 
 
 SPIRIFERA CURVATA, Schlotheim, P1. 37, figs. 3-5, 7. 
 
 Anomia Terebratulithes curvatus, Schl., Nachtriige zur Petrefact., 1882, p. 68, t. 19, f. 2. 
 Spirifera curvata, Davidson, Mon. Brit. Dev. Brach., 1864, Pt. 1, p. 39, t. 4, f. 29-22; t. 9, f. 22, 26, 26a, 
 27, 27a-c (for synonymy). 
 5 5} Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 269. 
 
 Obs. A full description of this species by the late Dr. T. Davidson will be found 
 in his work quoted in the synonymy. 
 
 * Petrefacta Germanie, 1826, I. Theil, t. 29, f. 3. - 
 + Tabulate Corals Pal. Period, 1879, p. 112. 
 + Foss, Pal. Nouv.-Galles du Sud., 1876, Pts. 1, 2, p. 76, t. 3, f. 1. 
 
65 
 
 In the Queensland examples the sulcus of the ventral valve channels the umbo 
 high up, and gradually broadens out towards the front, which is well sinuated. The 
 fold of the dorsal valve is not high, but narrow and ribless, except at the front sinuated 
 margin, where it rather projects upward. The hinge line is less than the width of the 
 valves, the area of the ventral valve being short and low, whilst the alar angles are 
 rounded. Both beaks are fairly prominent, and that of the ventral valve incurved. 
 The surface always appears quite smooth. 
 
 The narrow sinus and fold and the channelling of the ventral umbo just referred 
 to are well shown in Dr. Davidson’s figures of European specimens, and serve to 
 strengthen the identity of the respective fossils. 
 
 The crushed condition of the specimens on which the present identification was 
 originally made, left room for some doubt. Additional examples, however, quite 
 confirm the presence of S. cwrvata in the Queensland Devonian fauna. These, as 
 above stated, are smooth, but this results simply from the state of preservation, for it 
 must not be forgotten that on the original example there were traces of the character- 
 istic concentric imbrications, with the peculiar vertical serrations crossing them. 
 
 In general habit §. cwrvata resembles some small examples of the Carboniferous 
 Martinia glabra; and again 8S. levis, Hall,* of the Portage Group (Upper Devonian) 
 of North America. 
 
 Loc. Fanning River, and Fanning Old Station, Burdekin Downs. (&. L. Jack.) 
 
 SPIRIFERA EURYGLOSSA, Schnur, Pl. 4, fig. 1. 
 
 Spirifer curyglossus, Schnur, Palaeontographica, iii., p. 209, t. 36, f. 5 a-d. 
 
 Spirifera euryglossa, Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 269, t. 7, f. 1. 
 
 Obs. Another Spirifer occurs in the Fanning Limestone, of which we at present 
 have only one specimen, It is quite decorticated, much smaller than the preceding, with 
 a deep well-pronounced sulcus in the ventral valve extending well up on the beak, and 
 bounded by strong ridge-like margins. In the dorsal valve there is a corresponding 
 medial fold although not relatively so prominent as the sulcus. The hinge line was less 
 in length than the width of the shell. It appears to resemble some of the Martinia 
 glabra group, but the loss of the shelly matter renders identification difficult, especially 
 as we have only one specimen. A close resemblance exists between Spirifera euryglossa, 
 Schnur, and the present species. 
 
 Loc. Fanning River, Burdekin Downs. (2. Z. Jack.) 
 
 Family—ATRYPID. 
 
 Genus—ATRY PA, Dalman., 1828. 
 (Kongl. Vet. Acad. Handl. fér ir, 1827, p. 102.) 
 
 ATRYPA RETICULARIS, Linncus, Pl. 4, fig. 4. 
 Anomia reticularis, Linn., Syst. Nat., 1776, 12th Ed., i., Pt. 2, p. 1152. 
 Atrypa reticularis, Davidson, Mon, Brit. Dev. Brachiopoda, 1864, Pt. 1, p. 53, t. 10, f. 3, 4 (for synonymy). 
 a ae Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 270, t. 7, f. 2. 
 ae 95 Foord, Geol. Mag., 1890, vii. (3), p. 100, t. 5, f. 1, and woodcut, f. a, 0. 
 
 Obs. Numerous specimens of this world-wide species have now been collected 
 in North Queensland, supporting the original determination made by the Writer. There 
 
 
 
 * Pal, N. York, 1867, iv., Pt. 1, t. 39, £. 1-12, 
 
66 
 
 can be little doubt that A. reticularis is a very characteristic shell of the Fanning 
 Limestone. The larger number of the specimens are a good deal weathered, but in the 
 original example “the characteristic decussating frills or lamine are preserved on both 
 valves, but they are seen to much greater advantage on the ventral valve.” One of the 
 recently collected specimens, apparently of this species, shows traces of the spines 
 around the broken edges of the shell. 
 
 The only apparent real difference between this species and the next, is the 
 presence of the area in the latter. This however, varies much, both in length and 
 height, and at times is even very difficult to distinguish. Indeed, from an examination 
 of these specimens I can quite understand the late Dr. Davidson’s difficulty, expressed 
 in the following words—“‘I am very uncertain whether Atrypa desquamata be really 
 
 more than a variety of A. reticularis.” 
 Loc. Fanning River, Burdekin Downs, and Fanning Old Station. (&. L. Jack.) 
 
 ATRYPA DESQUAMATA, J. de C. Sowerby, Pl. 4, figs. 2,3; Pl. 37, fig. 8. 
 Atrypa desquamata, J. de C. Sby., Trans. Geol. Soc., 1840, 2d. Ser., v., Expl. of t. 56, t. 56, f. 19, 20. 
 Davidson, Mon. Brit. Dev. Brach., 1864, Pt. 1, p. 58, t. 10, £, 9-13, t. 11, f. 1-9 (for 
 synonymy). 
 Xf; Pr Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 270, t. 7, f. 3, 4. 
 
 Obs. From the series of figures of Atrypa desquamata given by Dr. Davidson, 
 it is quite clear that the species is one of considerable variation, both in the relative 
 dimensions of the shell, from the hinge line or beak to the front margin, and also 
 laterally, from side to side, the result being that the length of the hinge line is also 
 variable, short in some varieties, longer in others. 
 
 We possess several shells from the Fanning River Beds which are more 
 than probably this species. If we take the best preserved of these, we find that 
 it is very much more transverse than those represented by Dr. Davidson on Pl. x. 
 of his Devonian Monograph, but not more so than some of the figures of Pl. xi. 
 of the same work. Again, the relative convexity of the valves when in apposition 
 is very much less than Dr. Davidson’s fig. 1b of PI. xi., but is a little more pronounced 
 than the fig. 8a of the same plate. Even among the three Queensland examples 
 the shape varies somewhat. The ribbing of the valves corresponds with that seen 
 in A. desquamata, and there are also traces of concentric lamine. The above Author 
 laid stress on the exposure of the foraminal aperture and presence of an area. Both 
 are to a certain extent visible in one of the earlier specimens collected. In one of 
 the more recently acquired examples the beak of the ventral valve is very acute and 
 prominent. The strength of the surface coste or ribs is not in every case equal, 
 some being much more prominent and pronounced than others. The ventral valves 
 are gently but regularly curved, and there is a moderately pronounced sinuation in the 
 front margin. 
 
 Professor McCoy appears to have been the first to describe* the spiral 
 appendages in A. desquamcta, and they have since been figured in their entirety 
 by Dr. Davidson.t It is interesting to note that two of the specimens under 
 description exhibit traces of these appendages from the shell having been removed by 
 weathering. 
 
 Loc. and Horizon. Limestone of the Fanning River, and shale above the Fanning 
 Limestone, at Fanning Old Station, Burdekin Downs. (R. LZ. Jack.) 
 
 > 29 
 
 
 
 * Brit, Pal, Foss., 1852, Fas. 2, p. 379. ot OC Clbse Use le kent sess 
 
a? 
 
 
 
 67 
 
 Family—RHYNCHONELLIDA, 
 
 Genus—RHYNCHONELLA, Fischer, 1809. 
 (Notice Foss. Gouv. Moscou, p. 35.) 
 
 RHYNCHONELLA PRIMIPILARIS, Von Buch, Pl. 4, fig. 5. 
 
 Terebratula primipilaris, Von Buch, Phys. Abhandl. K. Akad. Wissensch. Berlin, 1835, p. 88, t. 2, f. 29 a-¢ 
 Rhynchonella primipilaris, Davidson, Mon. Brit. Dev. Brach., 1865, Pt. 2, p. 66, t. 14, f. 4-6, 
 “5 sp. ind., Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 271, t. 7, f. 5. 
 
 Obs. Several Rhynchonelle from the Fanning horizon have given much trouble 
 from the state of their preservation, which is unsatisfactory, but they appear to corres- 
 pond better with the characters assigned by Dr. Davidson to Von Buch’s species than 
 to any other. The shape of the shell appears to be much the same, and the bending 
 down of the front margin of the dorsal valve is quite apparent in all the specimens. 
 On submitting the specimens to Dr. Davidson he replied that ‘the Rhynchonelle seem 
 to be very close to the R. primipilaris of the Devonian.” 
 
 Loc. and Horizon. Fanning Old Station, Burdekin Downs, in shale above the 
 Fanning Limestone. (2. L. Jack.) 
 
 Genus—PENTAMERUS, J. Sowerby, 18—. 
 (Min. Con. i., p. 73.) 
 
 PENTAMERUS BREVIROSTRIS, Phillips, Pl. 37, figs. 6, 9-11. 
 Stringocephalus brevirostris, Phillips, Pal. Foss. Cornwall and Devon, 1841, p. 80, t. 32, f. 143. 
 Pentamerus brevirostris, Davidson, Mon. Brit. Dev. Brach., 1865, Pt. 2, p. 72, t. 15, f. 1-14. 
 
 Obs. This is an exceedingly variable species, sub-orbicular, circular, or broad- 
 ovate ; the dorsal valve with or without a mesial fold, and sometimes even with a sinus ; 
 and the ventral valve evenly gibbous, or with a slight fold, and ornamented or not with 
 a few slight longitudinal ribs. 
 
 Amongst the Queensland examples is a specimen in which both valves possess 
 a mesial fold, and the front margin is a good deal sinuated; whilst in others the 
 ventral valve is quite plain; another in which the fold is faintly ribbed; and again 
 others in which the dorsal valve is itself without a fold. As regards form, we are 
 presented with the long sub-orbicular outline, the broad-ovate condition, and one 
 individual in which the shape is almost circular. Indeed, the various outlines accord so 
 well with those of European specimens as to be remarkable, the only difference 
 traceable being the less development of the area in the Australian examples, and the 
 consequent concealment of the fissure; this is, however, perhaps assisted by the greatly 
 incurved ventral umbones. A fractured example of the ventral valve shows the septum, 
 so characteristic of the genus, which is large and well developed. The shelly plates of 
 the same valve had no great degree of divergence. 
 
 Loc. and Horizon. Fanning Old Station, Burdekin Downs; Fanning Lime- 
 stone. (R. L. Jack.) 
 
 Family—STRINGOCEPHALIDZ. 
 
 Genus—STRINGOCEPHALUS, Defrance, 1827.* 
 (Dict. Sci. Nat., 1827, p. 102.) 
 
 STRINGOCEPHALUS P sp. ind. 
 
 Obs. A single very imperfect specimen has been obtained from the Fanning 
 Limestone, which I believe to be referable to this genus. It consists of a maltreated 
 
 
 
 * Emend. Sandberger, Neues Jahrb., 1842, 
 
68 
 
 ventral valve of a large Brachiopod, with indications of a long septum, a moderately 
 wide but not high area, and a particularly lofty umbonal region. Notwithstanding its 
 imperfect state it even now measures 3 inches square. 
 
 IT am not acquainted with any other Devonian shell of sufficient size to 
 be confounded with this, and have, therefore, provisionally referred it to Stringo- 
 cephalus. 
 
 Loe. and Horizon. Fanning Old Station, Burdekin Downs; Fanning Lime- 
 stone. (fH. L. Jack.) 
 
 Family—STROPHOMENID. 
 
 Genus—ORTH OTETES, Fischer, 1829. 
 (Bull. Soc. Imp. Nat. Moscou, 1829, p. 375.) 
 
 ORTHOTETES UMBRACULUM, Schlotheim. 
 
 Terebratulites umbratulum, Schl., Petrefactenkunde, 1820, p. 256. 
 
 Streptorhynchus umbraculum, Davidson, Mon. Brit. Dev. Brach., 1865, Pt. 2, p. 76, t. 16, f. 6; 
 t. 18, f. 1-5. 
 
 Spirifera crenistria, Phillips, Geol. Yorkshire, 1886, ii., p. 216, t. 9, f. 6. 
 
 Streptorhynchus crenistria, Davidson, loc. cit., 1865, Pt. 2, p. 81, t. 18, f. 4-7. 
 
 Orthotetes crenistria, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 212, t. 10, f. 8. 
 
 a + Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 272. 
 
 Obs. The late Dr. Davidson called attention to the questionable separation of 
 Orthotetes umbraculum, Schl., sp., and O. erenistria, Phill., sp., and explained how the 
 two species had been confused by Authors. It appears from his own showing to be a 
 multiplication of names, as no good line of demarcation exists between the so-called 
 species. 
 
 In the Queensland Devonian examples the ventral valve is convex, the interspaces 
 between the coarser ribs being occupied by from three to four finer ones. The dorsal 
 valve is flat, or a little concave. One of the specimens in its present state is quite 
 3 inches wide by 2 inches high, but when perfect was wider. On the other hand no 
 creat depth existed between the valves. Like typical forms of O. wmbraculum, the 
 present shells possessed a well-developed area. 
 
 Loc. Fanning Old Station, Burdekin Downs. (&. LZ. Jack.) 
 
 ORTHOTETES ? CONCENTRICA, sp. nov., Pl. 37, figs. 18, 14. 
 
 Sp. Char. Transversely semicircular, compressed, slightly curved, thin towards 
 the front. Ventral valve flatly convex above, becoming concave towards the front ; 
 umbo projecting outwards almost at right angles to the hinge line, and very sharp. 
 Dorsal valve slightly rounded in the umbonal region, and following the contour of the 
 ventral valve. Area large and triangular, almost flat. Surface of the ventral valve 
 with faint radiating lines, crossed by markedly concentric imbricating lamine, giving 
 rise to a dull reticulation. Dorsal valve ornamented in a similar manner, but the 
 concentric lamin predominating. 
 
 Obs. Thisis a peculiar and interesting little form, especially in the ornamentation 
 of the surface, which is not of a character usual in this genus. In outline it seems to 
 approach Streptorhynchus pectiniformis, Dav.,* of the Salt Range Group, India, more 
 than any other species. 
 
 Lec. Fanning Old Station, Burdekin Downs. (R&R. LZ. Jack.) 
 
 
 
 * Waagen, Pal. Indica, Ser. xiii., Vol. 1, No, 4, Pt. 3, t. 55, f. 4-11, 
 

 
 69 
 
 Class—CEPHALOPODA. 
 
 Order—TETRABRANCHIATA. 
 Family—NAUTILIDZ. 
 
 Genus—GYROCERAS, De Koninck, 1844. 
 
 Gyroceras, De Kon., Anim. Foss, Terr. Carb. Belg., 1844, p. 530, 
 ; Blake, Mon. Brit. Foss. Cephalopoda, 1882, Pt. i., p. 65, 
 
 Obs. Gyroceras is here used in the restricted sense as defined by Prof. J. F. 
 Blake. 
 
 GyRocerRaAs PuHItrt, sp. nov., Pl. 4, figs. 6, 7. 
 
 Sp. Char.. Shell large, of one and a-half to two whorls, somewhat irregularly 
 convoluted ; section of the whorls apparently scutiform, and depressed or flattened on 
 
 the ventral side ; diameter of the shell as preserved, 53 inches; chambers shallow for 
 
 size of the shell; septa, of which there are about fifty visible, appear to be excavated 
 towards the rear on the back and ventral side, and to be arched forward on the flanks— 
 at the younger end of the shell the septa average ¢-inch apart, but in the older portions 
 they are much closer; siphuncle moderately large, and dorsal in position; the back 
 was traversed in the direction of its growth by a number of sharp, parallel, semituber- 
 culate, spiral ridges; the younger portion of the shell, at least, appears to have been 
 ornamented by distant obtuse nodes on the sides overhanging the open umbilicus, 
 whilst both the nodes and the interspace between them carry very fine epithecal striz, 
 which describe the same curve as the septa. 
 
 Obs. This genus has not hitherto been recognised in the Devonian rocks of Aus- 
 tralia. The specimen from which the above description is drawn up is unfortunately not 
 entirely preserved, nearly one-half of the shell haying been removed longitudinally by 
 weathering. The body chamber is only partially preserved, to the extent of 12 inches. 
 G. Philpi bears some resemblance to G. ornatum, Goldfuss, as figured by G. and F, 
 Sandberger,* whose figure shows the same indistinct nodes on the sides, and the same 
 spiral ridges on the back, but G. ornatwm appears to have been a much more robust 
 species than ours. It again resembles G. nodosum, Goldfuss, as figured by Bronn,t in 
 the possession of the distant nodes at the sides, but does not appear to correspond with 
 the latter in the section of its shell. The species is named in honour of the discoverer, 
 Mr. John Philp, senr., of Townsville. 
 
 Loc. Philp’s, Northern Railway (&. L. Jack) ; Reid Gap, near Townsville (G4. 
 Sweet—Colln. Sweet, Melbourne) ; Fanning River, near Fanning Old Station (R. ZL. 
 Jack). 
 
 E. 
 
 
 
 * Versteinerungen Schichtens. Nassau, Atlas, t. 18, f. 1, 1a, 0. 
 + Lethea Geog., Dritte Auflage Atlas, t. 1, f. 4. 
 
CHAPTER VI. 
 THE PERMO-CARBONIFEROUS SYSTEM. 
 
 THE greater part of the stratified rocks of the eastern ranges of Queensland may be 
 grouped together in a system to which the name of Permo-Carboniferous may appro- 
 priately be applied. This system includes at least four, and possibly five, distinct 
 formations, namely—the Gympie, Star, and Lower, Middle, and Upper Divisions of the 
 Bowen River Coal Field. 
 
 The two first yield a flora in no way allied to that which is found in the three 
 succeeding divisions but possessing a decidedly Carboniferous facies, the distinguishing 
 plant being Lepidodendron. The plant beds are associated with a marine fauna, which, 
 indeed, preponderates largely over the flora in the Gympie Formation. 
 
 There is not, indeed, much to indicate whether the Gympie Formation is older 
 than the Star, or vice versd. Certainly no section has come to light revealing their 
 relation to one another. But from the fact that the strata of the Gympie Formation 
 (except in a limited area of the type district) are almost always highly inclined and to 
 some extent metamorphosed, while the Star Formation is generally little disturbed and 
 little altered, it may be surmised that the latter is unconformably related to the former; 
 and for the present it is desirable to keep the two formations distinct, although the 
 accumulation of paleontological evidence appears to be tending to bridge over the gap 
 between them. 
 
 J. 
 
 The three Bowen River Formations are distinguished both by the presence of a 
 copious marine fauna, partaking of a Carboniferous and Permian nature, and a flora from 
 which Lycopodiaceous plants are almost entirely absent, being replaced by others of a 
 less Paleozoic and more Mesozoic description. In the Middle Formation of the Bowen 
 River Coal Field we find a preponderating Paleozoic fauna, and the much-debated fern 
 Glossopteris scantily represented. On the other hand, in the Upper Formation of the 
 Bowen River Coal Field this fern assumes a prominent position, and the older fauna is 
 either absent or reduced to a minimum. The Lower and Middle Bowen Formations and 
 their representatives in New South Wales have usually been termed ‘“‘ Carboniferous.” 
 They do not, however, wholly correspond to that formation as developed in Europe, but 
 rather homotaxially represent both it and the overlying Permian Formation. Hence, 
 referring to the Queensland beds only, I some years ago* proposed to call this series of 
 beds Permo-Carboniferous. I still believe this to be the nearest comparison which can 
 be made, and am desirous of extending it to the whole of these deposits throughout 
 Eastern Australia. 
 
 The notably Carboniferous facies of the Lower and Upper Marine fauna of New 
 South Wales, and the Bowen, Gympie, and Rockhampton corresponding series, hardly 
 requires demonstration, whilst a resemblance to the Permian is brought out greatly by 
 such forms as Strophalosia, Stenopora, and large Polyzoa of the Protoretepora type, and 
 
 * Proc. R.. Phys. Soc. Edinb., 1880, v., p. 319. 
 

 
 71 
 
 by the strong resemblance of the typical forms of Productus to the characteristic P. 
 horridus of the Magnesian Limestone wud Zechstein. This subject was fully discussed 
 in my account of “ A Collection of Fossils from the Bowen River Coal Field,” &c.,* 
 wherein I concluded as foilows:—‘ The examination of these Bowen River fossils, so far 
 as it has gone, leads me to regard them as occupying a high position in the Paleozoic 
 Series; and that all purposes would best be served by regarding them as of Permo- 
 Carboniferous age.” This view has gained strength, the more the facts have been 
 investigated, and I am now anxious to extend the adoption of this term to the whole of 
 the similar formations in New South Wales. 
 
 One of the most important points of difference between the Carboniferous Series 
 of Europe and the coal-bearing rocks of Eastern Australia lies in the almost entire 
 absence of Lycopodiaceous plants from the latter, above a certain horizon very low in 
 the series. The place of this division of the Vegetable Kingdom is taken by the fern 
 Glossopteris, and the continuity of the whole strata, now proposed to be termed Permo- 
 Carboniferous, both in New South Wales and Queensland, is shown by the passage of 
 this genus from the Middle to the Upper Bowen Formation and its persistence therein.t 
 
 The strata of the Oakey Creek Coal Field, Cooktown, contain Glossopteris, and are 
 regarded by Mr. Jack as the equivalent of the Upper or Freshwater division of the 
 Bowen Series. The Little River Coal Field beds near Palmerville, and those of Stewart’s 
 Creek near Townsville, are in the same category. It will be noticed that throughout the 
 horizons regarded as the equivalents of the Upper Bowen Formation there is an entire 
 absence of the genera Tewniopteris and Thinnfeldia, both of which become eminently 
 characteristic of the Mesozoic Coal Measures described later on. It seems more than 
 probable that the occurrence of these genera will afford a reliable basis, not only in 
 Queensland, but equally so in New South Wales, for the separation of those strata 
 which I am desirous of terming Permo-Carboniferous, from the still higher series, a 
 portion of which, at least, are clearly of Jurassic age. 
 
 With the elaborate classification, extending from the Trias to the Jurassic, pro- 
 posed by the Revd. J. E. Tenison Woods,{ or the still more beautifully fitting strati- 
 graphical tabulation devised by Prof. O. Feistmantel,§ I cannot at the present moment 
 coincide. No fossil organic remains are so deceptive or unsuitable for determining 
 questions of equivalent stratigraphy, as plants, and we know too little, not only of the 
 boundaries of formations in this quarter of the globe, but also of their organic contents, 
 to warrant speculations of this kind. That we have beds of Triassic age, and others 
 again representing some portion of the Jurassic, is probably the case, but it is impossible 
 to enter into minute stratigraphical subdivisions yet, on the mere chance of statements 
 ultimately proving correct. 
 
 E. 
 
 
 
 * Proc. R. Phys. Soc. Edinb., 1880, v., p. 319. 
 
 + Glossopteris is not as yet known in any of the Queensland Mesozoic formations except, strange to say, 
 in the very uppermost division of the Desert Sandstone. 
 
 t Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. i., pp. 53, 54. 
 
 § Palaeontographica, 1878-79, Sup. Bad. iii. 
 
CHAPTER VII. 
 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 THE GYMPIE FORMATION IN THE TYPE DISTRICT. 
 
 Mineral Areas—viz., Gympie Gold Field and Neerdie Antimony Mine. 
 
 To aseries of strata which attain an immense development in the south-eastern portion 
 of the Colony, and are probably represented in many portions of the eastern coast 
 district to the North, we have given the name of the “‘ Gympie Beds,” from the gold- 
 field where they have, for the most part, been studied. To this series, so far as yet 
 known, we have neither recognised a base nora top. Its place in the geological scale 
 must therefore, for the present, be determined mainly on paleontological evidence. 
 
 The late Mr. D’Oyly H. Aplin, Government Geologist for South Queensland, 
 made a report to the Government “On the Geological and Mining Features of the 
 Gympie Gold Field”* in 1868. 
 
 Mr. T. R. Hacket, Mining Surveyor, published in 1870 a Geological Map of the 
 Gympie Gold Field, but was content to distinguish “ Greenstone,” “ Fossiliferous Green- 
 stone and Slate,” and “ Slate and Sandstone.” 
 
 Mr. Daintree, in his paper on the “ Geology of Queensland,” + made some refer- 
 ences to the “ Devonian” rocks of the Gympie Mining District, from which he made a 
 collection of fossils which were determined by Mr. R. Etheridge, F.R.S. Mr. Etheridge’s 
 list of fossils hardly bears out the reference of the strata to the Devonian. Of the 
 fourteen fossils specifically determined by him, six (viz., Ceriopora (7) laxa, Eth., 
 Spirifera dubia, Eth., Aviculopecten imbricatus, Eth., A. multiradiatus, Eth., Edmondia 
 concentrica, Eth., and #. obovata, Eth.) are species either new or doubtful; four (viz., 
 Productus cora, D’Orb., Spirifera bisucleata, Sby., Aviculopecten limeformis, Mor., and 
 Plcurotomaria carinata, Sby.) are European Carboniferous. One of the new species 
 (viz., Ceriopora laxa) is most nearly allied to an Irish Carboniferous species. Another 
 (Strophomena rhomboidalis, var. analoga, Phill.) ranges in Europe from Silurian to 
 Carboniferous; while only one (viz., Spirifera undifera, var. undulata, Romer.) is 
 exclusively Devonian. The balance of evidence, therefore, so far as it was before Mr. 
 R. Etheridge, F.R.S., appears to have been in reality much in favour of a homotaxial 
 relation with the European Carboniferous. ; 
 
 Mr. A. C. Gregory, in his “ Report on the Geology of Part of the Districts 
 of Wide Bay and Burnett,’{ gave a stratigraphical description of the Gympie Gold 
 Field. 
 
 The Rev. W. B. Clarke, in his “ Sedimentary Formations of New South Wales,’’§ 
 gave a list of fossils “ capable of identification,’ from Gympie. These fossils, however, 
 
 * Brisbane : by Authority: 1868. 
 
 + Quart. Journ. Geol. Soc., xxviii., p. 289 (1872). 
 {+ Brisbane: by Authority : 1875, 
 
 § Fourth Edition, 1878, p. 20. 
 

 
 73 
 
 received from Mr. Clarke only generic names, as follow :—WNucula, Fenestella, Solarium, 
 Spirifera, Orthonota, Edmondia, Stenopora, and Producta. In an Appendix* to Mr. 
 Clarke’s work, Prof. De Koninck added Spirifer Strzeleckii, De Kon., to the Gympie 
 list. 
 
 In the Chapter on the Devonian Rocks I have already given my reason for trans- 
 ferring large areas of the rocks hitherto regarded as Devonian to the Gympie Formation. 
 As an example of extreme metamorphism of stratified rocks, presumably of the Gympie 
 Formation, Mr. Samuel Stutchbury’s descriptiont of the Glasshouse Mountains in 
 Moreton Bay may be quoted in this place. 
 
 “The special forms and characteristics which the Glasshouse Mountains present 
 are peculiarly interesting. At first sight, hand specimens might be taken for a fine- 
 grained granite; but on examining these en masse and carefully viewing all the 
 attendant circumstances, there can be no doubt that they are metamorphic sandstones. 
 It is evident that no granite masses could have been projected in the form they now 
 assume; they must have been surrounded by some supporting material such as the 
 continuation or extension of the same strata would give, now removed by denudation. 
 Upon careful examination lines of stratification can yet be traced. The largest of the 
 mountains, ‘ Beerwah,’ presents precipitous faces, especially on the northern and 
 eastern sides, exhibiting semi-basaltic columns leaning trom the base towards the centre. 
 The sandstone rock adjacent is, in many instances, composed of minute crystals of 
 quartz, each crystal being slightly abraded. In other instances it contains mica (similar 
 to our Old Red Sandstone and Pennant Grits at home), and much ferruginous matter ; 
 whilst Beerwah itself appears in composition, as already stated, like a granitell with a 
 few crystals of albite superadded.”’ . . . ‘“ We can easily imagine that at a period 
 subsequent to the Coal Measures there were as many foci of heat as there are now 
 mountains, without the pyrogenous rocks having the power to burst through the 
 accumulated strata of sandstone (Beerwah being from 700 to 800 feet above the level 
 of the plain upon which it stands), but sufficient, by their heat, to induce a meta- 
 morphosis in the superincumbent sandstone, giving origin to the crystals of felspar, and 
 causing a solidification of the material, which has to a degree protected it ; while those 
 portions of the unchanged surrounding sandstones have been removed to the extent 
 observed between the level of the plains and the tops of the existing mountains.” 
 
 These same mountains have, however, been described by a later observer, the 
 Hon. A. OC. Gregory,t as “ remarkable outbursts of porphyritic rocks.” 
 
 The late Mr. D’Oyly H. Aplin noted in 1867 § the occurrence of branched corals 
 and crinoidal stems at Elbow Creek, Lucky Valley, in blue slates, within a series of 
 slates, sandstones, and calcareous grits. Above the slates Mr. Aplin noted also 
 calcareous grits with shells and casts of various Brachiopoda, Gasteropoda, and 
 bivalves. Of these only Productus and Spirifer were mentioned, even by their generic 
 names. Mr. Aplin regarded the fossiliferous series as Silurian, and remarked of the 
 fossils that ‘in general aspect they resemble the fossils of the diorite slates at Gympie,” 
 {p.5). To this latter statement I should attach greater weight than to the determination 
 of two genera of Brachiopods, which range up to a much later date than Silurian. I 
 could even believe, without difficulty, in the absolute identity of the Lucky Valley Beds 
 
 
 
 
 
 * Appendix xvi. “‘C,” p, 188. 
 + New South Wales Geological Survey. Fourteenth Tri-monthly Report, dated Durandin, 1st 
 August, 1854. Legislative Council Papers, N.S.W., 19th September, 1854. 
 
 + Report on the Geology of Part of the Districts of Wide Bay and Burnett. Brisbane: by 
 Authority : 1875. ; 
 
 § Report on the Auriferous Country of the Upper Condamine, &c, Brisbane: by Authority: 1867. 
 
74 
 
 with those of the Gympie Formation, especially as similar slates containing corals and 
 crinoid stems have proved to be quite characteristic of the Gympie Formation, as 
 developed in the Rockhampton District. 
 
 Mr. A. C. Gregory, in his “ Report on the Geological Features of the South- 
 eastern Districts of Queensland,’’* refers to casts of Spirifer “found in the Devonian 
 slates and sandstones,” at Lucky Valley and the head of Rosenthal Creek, “and also in 
 the limestones and other beds of this series near Rockhampton.” 
 
 From this meagre evidence, I regard the slates, &c., to the west and south of 
 Warwick as belonging to the Gympie Formation rather than to the Devonian. 
 
 Mr. Aplin, in the report above quoted, frequently refers to the lithological 
 resemblance of the slates, &c., of the Moreton Bay District, north of Brisbane, to the 
 Gympie rocks, which, although he regarded them as Devonian, are now relegated to the 
 Permo-Carboniferous. Abundant evidence will be noted in the following pages in 
 favour of transferring the greater part of the stratified rocks between this region and 
 Rockhampton, from the Devonian to the Gympie Formation. If these slates, &., are 
 of Permo-Carboniferous age, it is probable that so likewise are the slates, schists, and 
 quartzites extending from Brisbane to the Border; but in the meantime, in the absence 
 of direct evidence, these are still left on the map as of “ undetermined age.”’ 
 
 As in all probability the strata on the New South Wales side of the Border, 
 provisionally mapped as “ Upper Silurian or Siluro-Devonian,” are continuous with 
 those of Lucky Valley, we look to the work of New South Wales geologists in that 
 region for light on the subject. Mr. (now Professor) T. W. Edgeworth David, in his 
 exhaustive Memoir on the “ Geology of the Vegetable Creek Tin-Mining Field,’f in 
 referring to some Polyzoa, Encrinites, Lamellibranchiata, and univalves found by him in 
 the Parish of Arvid, confesses (p. 54) that ‘“ these fossils prove the beds to be of marine 
 origin, but do not afford conclusive evidence as to their age.” 
 
 The Writer in 1886 made a partial survey of the Gympie Gold Field, and a large 
 collection of fossils. The Geological Survey Museum and the Queensland Museum 
 both contain a considerable collection of fossils from the same locality. 
 
 As my Colleague has carefully gone over the collections and the whole litera- 
 ture of the Paleontology of the Gympie Gold Field, it is unnecessary for me to allude 
 here further to the very puzzling lists of fossils furnished by early writers. The 
 stratigraphical information also furnished by the Authors above referred to, although 
 in many instances valuable, may be regarded as superseded, or added to and brought 
 up to date, by the exhaustive Report of Mr. William H. Rands, “On the Gympie 
 Gold Field.” ¢ 
 
 The most important part of the Gympie Gold Field (see Geological Map, Pl. 48) 
 is comprised within a strip of country on the northern bank of the Mary River, about 
 two miles in length, with an average breadth of about three-quarters of a mile, extending 
 from the town of Gympie southward to the Monkland. This area, it will be seen from 
 the map, is bounded on the north, south, and west, by faults. “This part of the field 
 presents a series of alternations of different kinds of sedimentary strata with some 
 intrusive igneous rocks, and also some of volcanic origin. Taking the average dip at 
 22°, there must be somewhat over 2,000 feet in thickness of such strata. 
 
 “The rocks of which these beds are composed consist chiefly of greywackes, 
 altered sandstones, grey and black carbonaceous shales, grits, conglomerates, breccias, 
 
 and limestone. Interbedded with these are amygdaloidal volcanic rocks and volcanic 
 ee a ee 
 * Brisbane : by Authority: 1879, p. 7. 
 + Mem. Geol. Survey N. 8. Wales, Geology No. 1, 1887. Sydney : Government Printer, 
 }~ Brisbane: by Authority : 1889, 
 

 
 75 
 
 ash. There are also sheets of an intrusive ‘ greenstone,’ which has undergone great 
 alteration. Most of the sedimentary rocks are more or less pyritous, some of the shales 
 especially being full of small cubical crystals of iron pyrites, and most of them, too, 
 are calcareous. This is especially the case with the sandstones, greywackes, and con- 
 glomerates, and with some of the shales. The faces of the ‘joints’ or cracks in the 
 rocks are almost invariably coated with carbonate of lime in the form of calcite. 
 
 “The strata dip with great regularity at an average angle of from 20° to 22°. 
 On the northern portion of the field the direction of dip is, as a rule, a little to the 
 north of east ; on the southern portion it is to the E.S.E. 
 
 “While many of the rocks have undergone but little alteration, others have been 
 greatly altered, almost to the obliteration of their original character. These rocks have 
 become indurated and in some cases semi-crystalline, and it is only with difficulty that 
 the latter can be distinguished from the true igneous rocks. Speaking generally the 
 rocks which occupy the lowest position in the series, and whose outcrops occur, there- 
 fore, at the western portion of the field, have undergone the greatest alteration ; 
 although in the upper part of the series rocks which have been considerably altered 
 alternate with those which have undergone but slight alteration. 
 
 “Perhaps the most typical section of the Gympie rocks is that which is taken 
 in a line (A-B) across the field from near the Railway Station to near Channon-street 
 Bridge (Pl. 54, 55). In the following list of rocks in the section the thicknesses 
 have been calculated from the outcrop of the strata at the surface, as very little mining 
 is going on now in this part of the field, and the old workings are generally inaccessible. 
 The figures are therefore only approximate, and the thicknesses vary greatly on either 
 
 side of the line of section :— 
 Ft. 
 
 = 
 =] 
 
 Blue impure limestone oralitercnsy : an 1s 2188.6 
 Coarse pebbly conglomerate with sandstone G ery thick ) Station) = 800, 0 
 Laminated pardstone ie uy Be Ate 7 uy rc ee Oo oO 
 Shales (fossiliferous) o : | f 56 4 
 Coarse altered conglomerate ... iia ee OS og ae LO ° Oo 
 Shales with beds of thin-bedded Lah Wie a caer Core cies 4 50 0 
 2 ft.4in. thick) | 
 
 Hard grey greywacke Ee a ee | | 20 O 
 Shales (fossiliferous) ... bss ce as aon L 66 O 
 Coarse pebbly conglomerate... vat ate aad ars ue apne ei P| 
 Laminated fine-grained sandstone ... ae a es Seek Zt) ot) 
 Angular grit (probably a volcanic agglomercte) av ses Sa. Sas reo Se 
 BAA and highly fossiliferous sandstone.. ee a <<. sy eh 
 Greenish semi-crystalline greywacke... Sis ive a eh see wag ine S5) 
 Shales, so-called ‘ First Bed of Slate’ a a? in oan “Fpl ey’ 
 Hard grey greywacke ... ra: ES. ne ew os eS 
 Coarse altered conglomerate ... x me abe a vr eee 20°20 
 Greenish semi-crystalline greywacke... aoe 5a: e. site eet LOeG 
 Sandstone and coarse altered conglomerate ... aie ae ee Pie GU) lead 
 Shales, so-called ‘ Second Bed of Slate’... oF ieee Log cl 
 Hard altered crystalline greenstone—‘ Gympie greenstone’ 8 Pied a 
 Green and purple altered chloritic rock; partly amygdaloidal volcanic 
 
 rocks, partly volcanic ash, and partly peranded a : EMP 
 So-called ‘Third Bed of Slate’ with a thickness of grey- green, fine- 
 
 grained greywacke, and underneath altered chloritic rocks like those 
 
 above iss ry bee ve we oF ¥,) wae oe 200 
 Limestone... a ints ra, ots ela ay és ah et pace 
 
 1,909 0” 
 
76 
 
 At the Monkland the bed of impure limestone which lies at the top of the auri- 
 ferous series “is considerably over 200 feet thick (probably about 230 feet). It can be 
 seen in the high northern bank of the river close to the small gully on the No. 2 Great 
 Eastern ground, but beyond that point I have been unable to trace it in a southerly 
 direction. The conglomerate that underlies the limestone is exceptionally thick where 
 the section-line crosses it. It is made up of pebbles ranging from 1 inch up to 8 inches 
 in diameter, and consisting chiefly of greywacke, sandstone, and quartz. In places 
 it passes into sandstone. 
 
 “T now come to the consideration of the beds of ‘ Black Slate,’ in connection with 
 which the richest deposits of gold have been found in the reefs. In the true sense of 
 the term these beds are ‘shales,’ and not ‘slates,’ the fissility or lamination coinciding 
 with the planes of bedding. 
 
 “The shales are at times laminated, sometimes thin-bedded, but generally thick- 
 bedded. They pass in places into aluminous sandstone, locally called ‘ Black Rock.’ 
 The. shales are carbonaceous, slightly caleareous (their joints are always coated with 
 calcite), and generally they are pyritous. Thin sections examined under the microscope 
 show them to be made up of fine carbonaceous mud, with small rounded and a few 
 semi-circular specks of quartz and small cubes of iron pyrites. 
 
 “There are four well-definel zones of slate. The uppermost one, which may 
 be termed ‘ Phaniz or Monkland Slate, is about 200 feet thick; in it there are a 
 few thin beds of sandstone and greywacke. By far the greater part of the gold 
 has been taken from the reefs when passing through this bed, in which fossils are 
 very numerous, the commonest forms being—Fenestella, Protoretepora, Spirifera, 
 Productus cora, Strophomena rhomboidalis, Aviculopecten, Pleurotomaria carinata, and 
 Orthoceras. 
 
 “The next beds of auriferous shale in descending order are what have been 
 termed by the miners the ‘ First and Second Beds of Slate.’ These beds vary from 
 10 to 20 feet each in thickness, and are about 100 feet or more vertically apart. They 
 are rich in iron pyrites, and are generally of a fissile structure. On weathering, they 
 become friable and brown in colour, owing to the amount of ferruginous matter in 
 their composition. Very rich deposits of gold have been obtained from reefs in 
 contact with these shales, especially during the early days of the field. The Lady 
 Mary, Caledonia, California, New Zealand, Crown, March, Hilton, and Hamburg Reefs 
 carried rich gold in these beds. So far as my observation went, these two beds are 
 not fossiliferous. 
 
 “The ‘ Third Bed of Slate’ lies about 400 feet below the second. It is quite 
 different in its character from that of the three zones lying above. It is always, too, 
 associated with a greenish-grey, fine-grained, laminated greywacke, possessing a flinty 
 or splintery fracture. This greywacke is of great thickness. The Ellen Harkins shaft 
 has passed through over 300 feet, and the Wilmot shaft about 200 feet of it. Thin 
 sections of this greywacke show, under the microscope, a very fine-grained ground-mass, 
 with small rounded and subangular particles throughout it. Beds of the black carbon- 
 aceous shale occur at various depths in this greywacke, three such layers occurring in 
 the Ellen Harkins; but besides these distinct beds there are patches of a black rock in 
 it, which, under the microscope, show a similar structure to the greywacke ; it is in fact 
 a black carbonaceous greywacke, the one rock passing insensibly into the other. The 
 whole thickness of greywacke and shales forms the fourth auriferous zone, and is known 
 on the field as the ‘Third Bed of Slate” The gold in this bed is exceedingly patchy, 
 and many claims have been working on it without success. It was, however, in this 
 shale, at a depth of 600 feet, on the Ellen Harkins Reef, that perhaps the richest patch 
 
——— 
 
 
 
 we 
 
 of gold yet met with on Gympie was obtained. In the outcrop of this bed, on the south 
 side of the river near the No. 2 South Ellen Harkins, the fossil Protoretepora ampla 
 occurs. This is the only spot in which I have seen fossil remains in this bed. 
 
 “ Another bed of slate is reported to exist below this, in one or two claims—The 
 Eldorado for instanece.’’ Mr. Rands was, however, in some doubt about its occurrence. 
 
 “A point of great interest is the occurrence of large isolated boulders in the 
 Upper or Thick Bed of Shale. As examples of these, I may mention one from the 
 No. 1 North Phoenix at a depth of 370 feet, at a point where the shale has passed into a 
 fine aluminous sandstone. This boulder consists of a fine siliceous greywacke, and its 
 dimensions are 13 x 10? x 5 inches. Another, in the shale in the Phenix Golden Pile, 
 is of a coarse greywacke, containing ill-defined erystals of felspar and crystals of iron 
 pyrites ; this was 8} x 5} x 34 inches. It would be difficult to say how far these 
 boulders have travelled, since these greywackes are not only common on the field itself, 
 but also throughout the Carbonifero-Permian and Devonian Rocks, which occupy a large 
 area in this district. The presence of such boulders iu a rock which was laid down as a 
 fine silt would point to the conclusion that they were dropped from floating ground-ice, 
 for any current of sufficient strength to carry along these boulders would have washed 
 away the lighter materials of which the shale is composed. 
 
 “A curious rounded boulder of granite, about 6 inches in diameter, was found 
 enclosed in the O’Connell Reef, in the O’Connell Prospecting Claim, at a depth of 
 240 feet. The granite is coarse in the grain, and is composed of pink orthoclase and 
 quartz, with a few specks of decomposed mica. This boulder must have been introduced 
 into the reef from the surface while the fissure remained open. It must have travelled 
 some miles, for I know of no granite nearer than that of the Black Snake Range, 
 which is about 20 miles west of Gympie.* The granite of which the boulder is 
 composed is very different to that from the rauge, being much coarser and containing 
 much more quartz. This is the only instance of a boulder of the kind having been 
 found. It is probable that at the time it was deposited the country was submerged, and 
 that the boulder was carried, probably on floating ground-ice, and dropped into the 
 position in which it was found, while other similar boulders, which would have been 
 dropped on the sea-bottom, have since been removed by denudation. Had it been 
 conveyed by any land stream, the fissure in the reef would probably have been filled up 
 with others brought along with it. 
 
 “The greenish fossiliferous sandstone just above the ‘ First Bed of Slate’ can 
 be traced from White’s Gully to the Lucknow, and then again at the Two-Mile. It is 
 a bed easily recognisable, serving well in determining the horizon of beds nearit. In 
 some places it is one mass of fossils. Amongst these are—AStenopora, Protoretepora, 
 Fenestella, Spirifera, Conocardium, Aviculopecten multiradiatus, Edmondia, Pleuro- 
 tomaria carinata, &e. 
 
 “The ‘ Gympie Greenstone’ is below the ‘Second Bed of Slate.’ As it has 
 been such a stumbling-block to the miner I must allude to it at some length. The 
 occurrence of gold in rocks below it has frequently been spoken of as contrary to all 
 preconceived ideas and principles, and the late Mr. Aplin’s Report is quoted in support of 
 this. Mr. Aplin says in reference to this ‘ greenstone’ :—-‘ Whether in irregular-shaped 
 masses or broad dykes, this rock occurs at intervals over a large portion of the area of 
 this goldfield, but it is most prominently developed within a zone of half-a-mile in width, 
 having a longitudinal direction of N. 60° W., and embracing the space from the Lady 
 Mary hill to that on which the Gympie township commences. It is in the decomposed 
 
 
 
 * “T have seen granite near Glastonbury, about 10 miles from Gympie, but it is of a different 
 character to that of which this boulder is formed,” 
 
78 
 
 portions of this rock, which weathers brown and becomes argillaceous, though main- 
 taining its compactness, that the quartz veins traversing it are found to be so highly 
 productive. In its ordinary condition it is excessively hard and is the most formidable 
 obstacle the miners have to contend with, some from the very surface, and others at 
 varying but at comparatively shallow depths.’* And further on in the same report he 
 says:—‘Up to the present time scarcely any of the reefs have been opened up to a 
 greater depth than between 60 and 70 feet, and but little stone has been raised below 
 30 or 40 feet within the limits of the belt of greenstone to which I have before referred. 
 From the crystalline character and extreme hardness of this rock, which I do not think 
 is likely to become softer as it is followed downwards, there is little probability that the 
 reefs traversing it can be profitably mined to any great depth, in fact in one or two 
 cases the tendency to become narrowed, and impoverished also, is already apparent ; and 
 though, perhaps, they may not be altogether “pinched out,” the quartz veins will, 
 doubtless, become so attenuated that it will be no longer profitable to work them.’ 
 
 “Mr. Aplin’s remarks with reference to the unproductiveness of the reefs in the 
 ‘oreenstone’t+ have been fully borne out by later experience, since none of the reefs 
 contain payable, if any, gold at all, when passing through it. The mistake he made was 
 coming to the conclusion, without sufficient evidence, that the greenstone was in the 
 form of ‘an irregular-shaped mass or broad dyke,’ whereas future development has 
 proved it to be in the form of an intrusive ‘sheet.’ Had it existed as a dyke or 
 irregular mass, one would have expected it to extend to any depth that the miner could 
 have reached, and it would have been useless to have attempted to follow the reefs into 
 it. The miner, in the early days, abandoned the reefs as soon as the greenstone was 
 reached, and he added also to his difficulty by calling every rock ‘greenstone’ which 
 was of a green colour. 
 
 “Tt was not for some years, when the upper levels were nearly worked out, that 
 deeper sinking was, at last, resorted to, and that auriferous beds were found lying 
 beneath the greenstone. In the case of an igneous rock, such as this, intruded in the 
 form of a ‘sheet,’ parallel with the planes of bedding, there is no reason why beds 
 favourable to the occurrence of gold should not exist below as well as above it. The 
 greenstone is intimately associated with other rocks which are, undoubtedly, of sedi- 
 mentary origin, but which have by alteration become so semi-crystalline that it is at times 
 difficult to distinguish between them. 
 
 “‘ Doubts have been expressed as to whether the greenstone is an igneous rock at 
 all; however, from its relation to the surrounding rocks, and the baked appearance some 
 of the rocks in contact with it have, there can be little doubt but that it is of igneous 
 origin, and that it is an intrusive sheet which, while generally conforming to the bedding 
 of the rocks, at times, both at its upper and under surfaces, break across their planes of 
 bedding. This feature can be well seen in the Smithfield United and the No.5 North 
 Glanmire Claims. The ‘greenstone’ varies from a dark to a cabbage-green in colour ; 
 it is very hard and breaks with a somewhat conchoidal fracture. In the microscope, 
 erystals of plagioclase felspar are discernible ; also very much altered greenish crystals, 
 either altered hornblende or augite, changing into viridite; opaque crystals of iron 
 pyrites and small grains of magnetite. The rock has undergone too much alteration to 
 name it definitely. It was probably either a diorite or dolerite. 
 
 * Report from the Government Geologist for South Queensland on the Geological and Mining 
 Features of the Gympie Gold Field. Brisbane: by Authority : 1868. 
 
 + Mr. Rands seems to have misunderstood Mr, Aplin’s remarks, which distinctly imply that the reefs, 
 so far from being unproductive, were most productive when traversing the greenstone, or at least its 
 decomposed portion, Mr, Aplin, however, was greatly in error as to the fact. (R.Z.J.) 
 

 
 79 
 
 “ Analyses of this ‘greenstone’ are given by Mr. Daintree in his paper on the 
 “Geology of Queensland,’’* and by Professor Liversidge.t They are :— 
 
 
 
 
 
 
 
 
 
 DAINTREE. LIVERSIDGE. 
 Per cent. Per cent. 
 Silica ... - te ve ms ... §0°500 A §4°952 
 Alumina he ik ah ote ... 18°485 ae 16°643 
 Ferric oxide ... or ip ae ee 47.0 ae 2°410 
 Ferrous oxide = ee eee .. 6°440 a 7849 
 Lime ... an ys a ae ... 8°800 fie 8645 
 Magnesia oe a Sar atid SOOO ne trace 
 Potash ae ae a mi ae) .0°635 rt, 1540 
 Soda ... He be aie dd iietec 8655 en 6°647 
 Sulphur ee eee ae be me aE! ee 
 Manganese protoxide ni “Age ‘ me ars trace 
 Carbonic acid ee a Bae oe 
 Water (constitution) one ae ine vein | By diff. 1°314 
 Water (hygroscopic) bes 5 ... 0°850 
 99:975 100°00 
 Sp. gr. 2°752 Sp. gr. 2°860 
 
 “Mr. Allport, of Birmingham, to whom Mr. Daintree referred this rock for 
 microscopic examination, says:—‘ This is diorite, containing hornblende, triclinic 
 felspar, a little brown mica (biotite), and pyrites.’ 
 
 “The micro-photograph of the section in Professor Liversidge’s paper shows a 
 rock made up of particles of other rocks, with fragmentary crystals of felspar, augite, 
 and magnetite, mingled with chlorite. This section does not resemble those cut by 
 myself and described above; and I am under the impression that the rock described by 
 Professor Liversidge as an altered ash or breccia is one of the green fragmentary 
 rocks. 
 
 “Although the reefs actually in contact with the ‘greenstone’ have become 
 impoverished, and do not contain gold in payable quantities, it nevertheless appears to 
 have had a favourable influence on the auriferous character of the shales in its vicinity, 
 for it is only in these beds that the reefs have contained payable gold. 
 
 “The reefs, in the great mass of shales which lie above, and to the east of the 
 upper bed of limestone, have not, so far, proved payable ; and, so far as my observation 
 goes, these shales are, with the exception of one or two small dykes and sheets of 
 diorite and porphyry, entirely free from intrusive igneous rocks. 
 
 “* Above and below the lower or third bed of shale, there is, as seen in the section, 
 a great thickness of altered greenish and purple chloritic rocks. I have examined the 
 rocks carefully, and find that many of them are of volcanic origin; some of them are 
 fragmentary (altered ash or breccia); others have been ejected in a molten condition, 
 as in the case of a purple and green amygdaloidal rock, which is met with in many 
 parts of the field. I examined a thin section of this rock under the microscope, and 
 would pronounce it to be an amygdaloidal diabase, very much altered ; the cavities are 
 generally filled with carbonate of lime, but sometimes with hydrous silica. In the Lady 
 Flora, small specks of native copper have been seen in this rock, at a depth of about 
 140 feet. The speck of copper in a specimen I found on the mullock heap was 
 surrounded with oxide of iron. The copper may have been reduced from either the 
 sulphide or oxide of copper by reducing gases given off during the cooling of the rock. 
 
 
 
 * Quart. Journ. Geol. Soc., xxviii., p. 293. 
 + Journ. R, Soc, N. S. Wales, xvi., p. 45. 
 
80 
 
 “Below these rocks, again, is a thin bed of bluish limestone, seen in Nash’s 
 gully, close to its mouth, near the river bank, in the Surface Hill shaft, and also on the 
 south side of the river near the Normanby Bridge. A few yards to the west of the 
 outcrop of limestone a thick mass of shales occurs, dipping very steeply to the south- 
 west, or in a direction just opposite to that of the Gympie rocks. These shales crop 
 out in the road cutting leading down to Channon-street Bridge. The shales would 
 appear to be outside of the auriferous area, no payable reefs having yet been found in 
 them. They are separated from the Gympie beds by a ‘strike-fault’ running nearly 
 north and south, the position of which is somewhere between the outcrops of the lower 
 bed of limestone and that of the shale in the road cutting. This fault makes all 
 chances of predicting what strata will be met with below the lowest known beds 
 impossible, for such strata, instead of cropping out at the surface, would come up 
 against the fault. 
 
 “The shales extend westwards for four or five miles, when they are covered by a 
 narrow belt of Desert Sandstone. ‘These shales are black in colour, but, unlike the 
 Gympie auriferous shales, they contain but little pyrites.” 
 
 One of the faults already mentioned is the “ Smithfield Crosscourse,” which 
 divides the area above described from the Monkland and Glanmire portion of the field 
 further to the south. It runs E. 16° N., and has a downthrow to the north of about 
 530 feet. “None of the reefs on the south side of this fault have been identified 
 with those on the north; on the south side, however, they would lie away to the west. 
 Taking the average underlie of the Phenix Reef at 27°, and allowing for a downthrow 
 of 550 feet, it would bring it nearly opposite the Ellen Harkins Reef, but it is impossible 
 to identify them with any certainty.” 
 
 On a line of section (E F, Pl. 57) drawn nearly east and west on the south 
 side of the Smithfield Crosscourse, ‘‘ We meet with a few marked changes, chief amongst 
 which is the absence of the first and second beds of slate. At some distance under- 
 neath the thick beds of limestone and pebbly conglomerate are the upper shales 
 identical with the Phoenix shales on the Phoenix line of reef; this is the bed in 
 connection with which the Smithfield, Columbia, Glanmire, Monkland, Great Eastern, 
 &e., &e., lines of reef have been worked; below the shales is an altered calcareous semi- 
 crystalline greywacke, then ‘greenstone,’ and below that again is the ‘Third Bed of 
 Slate,’ with its fine-grained greenish greywacke, with which it is always associated ; 
 the two thin beds, known as the ‘ First and Second Beds of Slate,’ which have been 
 worked in the Hilton, Golden Crown, and Nos. 7 and 8 South Lady Mary, &c., being 
 absent, unless the thin bed—in places not much thicker than a sheet of paper—in 
 which the rich gold was obtained in the Wilmot and Russell Reefs in the Wilmot 
 Extended Mine represents one of them. It is, however, of small extent, and has not 
 been traced south of that claim. The explanation of their absence appears to me to lie 
 in the fact that the two beds in question are thinning out to the east on the northern 
 side of this fault. The greywacke in which the ‘Third Bed of Slate’ occurs is thicker 
 here than on the northern part of the field. 
 
 “Still further south—that is to say, south of the South Ellen Harkins and Wilmot 
 Claims—we meet with another important change. Here the Third Bed of Slate has not 
 been met with on the northern side of the river, although the outcrop of this bed, or of 
 one very similar, may be seen a short distance west of the shaft of the No. 2 South 
 Ellen Harkins Leasehold, which is situated on the southern side of the river; so that, 
 up to the present, no auriferous beds have been met with in this southern portion of 
 the field below the thick Upper or Monkland Shales, and yet two of the deepest shafts 
 are situated in this part of the field—namely, those of the Inglewood and the Great 
 

 
 81 
 
 Monkland (Aurelia), which are down 1,200 and 1,300 feet respectively. Had it con- 
 tinued with its regular strike and dip, the ‘ Third Bed’ would have been met with in the 
 former shaft at a depth of about 750 feet, and in the latter at about 900 feet. The 
 country passed through in the two shafts is very similar, consisting chiefly of altered 
 stratified rocks of a grey or greenish colour. The lines of stratification are well 
 marked in the finer grained rocks. Some of the deepest rocks are very much altered 
 and are very chloritic, and resemble the lowest beds on the northern side of the field. 
 It is difficult to understand how the very great thickness of the fine laminated grey- 
 wacke, with shales, which occurs in the Union, the South Ellen Harkins and Wilmot, 
 the Ellen Harkins, the Wilmot Extended, &c., &c., would thin out and disappear 
 altogether in so short a distance ; and it is far more probable that a fault occurs between 
 the two points; if so, it must run in a direction so as not to disturb the Upper Shales, 
 for they are continuous throughout the Smithfield, Glanmire, and Monkland Claims. 
 The only direction that such a fault could run in would be about north-north-east, or 
 about parallel with that in the Monkland and Abyssinia. 
 
 ‘About thirty chains west of the Normanby Bridge the lower bed of limestone 
 can be seen for a short distance crossing Purcell’s selection.” 
 
 About two and a-half miles further south-east, near the Dawn Shaft, a bluish 
 limestone is seen. It can only be traced for a few yards, and the direction of its dip is 
 uncertain. ‘Immediately west of it are the thick masses of shale which occur every- 
 where west of the [auriferous]| Gympie beds. It would appear, therefore, that this 
 limestone must be a continuation of the lower bed.” . . . ‘The commonest forms 
 of fossils in this limestone are :—Protoretepora, Spirifera, Martinia glabra,* Avicu- 
 lopecten, and Productus brachytherus.t The only coral from Gympie {—a Cyathophyllum 
 —was from this bed.” 
 
 - “In the No. 2 South Ellen Harkins Leasehold the laminated greywacke with 
 bands of black shale—the Third Bed of Slate—is met with at a depth of 275 feet; east 
 of that are altered green and purple rocks, while a chain to the west of the shaft is the 
 outcrop of the beds of shale containing Protoretepora.” 
 
 North of the area whose structure has been illustrated by the first section (A B), 
 a strip of country about twenty-seven chains in width extends from the railway line near 
 the head of Commissioner’s Creek westward to Gympie Creek. This area is bounded on 
 the north and south by two parallel faults, the southmost having a downthrow to the 
 north and the northmost a downthrow to the south. Between these faults a cuneiform 
 mass of strata has been let in. The strike of the beds is parallel to the two faults—+.e., 
 forms an angle of 185° with the strike of the beds seen both to north and south. 
 “ These strata apparently belong to the overlying shales” [shales overlying the Gympie 
 auriferous rocks], “and consist of grey shales, with a bed of white crystalline limestone 
 in which the fossil Stenopora occurs numerously. This bed of limestone, therefore, not 
 only dips in a different direction, but is of quite a different character, and contains 
 different fossils to that which forms the upper part of the Gympie auriferous beds. A 
 similar limestone was cut in the shaft of the No. 1 North Lucknow, after passing 
 through 115 feet of laminated shales. These beds contained Strophomena rhomboidalis, 
 and Martinia glabra.”§ The dip of the strata between the two faults is about 15° 
 
 * Not included in my Colleague’s list, and therefore ignored. 
 
 + Not included in my Colleague’s Gympie list, but included in his list of fossils from Encrinite 
 Creek, Fenestella Hill, Stanwell, Kariboe Creek, and Yarrol = Gympie beds. 
 
 + Mr. Rands is in’ error here. He himself quotes Stenopora from above the ‘‘ First Bed of Slate,” 
 See antea, p. 77. (RE. junr.) 
 
 § Not included in my Colleague’s list, 
 
 E 
 
82 
 
 to S. Several shafts have been sunk between the two faults, but apparently to 
 no purpose, as the horizon of the strata met with was probably not recognisable owing 
 to the coming together of the two faults. 
 
 North of this area the upper limestone is again seen with its normal strike from 
 south-east to north-west, and a dip of 21° to 28° to N.E. Mr. Rands has mapped it 
 from this point continuously to a point about three-quarters of a mile east of O’Leary’s 
 Crossing of the Mary River on the Kilkivan road. 
 
 “A very cursory glance is sufficient to show that’? [at the Two-Mile] (see PI. 
 58) “we are dealing with very similar beds” [to those of the Central District, Gympie], 
 “while a closer examination shows that the order of superposition of the principal beds 
 is the same in both places, and that the strata of the Two-Mile are an actual continuation 
 of the Gympie Beds.” * 
 
 “The strata dip to E.N.E. at an average of about 20°. [See Section AB, Pl. 54, 
 55.] Beneath the thick mass of shales which lie away to the east we have, as 
 on Gympie, the bed of impure limestone, here about 150 feet thick. Immediately 
 below this is the bed of coarse pebbly conglomerate, with some thin beds of sand- 
 stone. Below this again can be seen the outcrops of shales with beds of laminated 
 sandstone—the equivalent of the ‘Upper or Phenix Slates’; then, at some distance 
 below this, is the greenish and highly fossiliferous sandstone, identical with and contain- 
 ing the same species of fossils as the bed which, on Gympie, is traced from White’s 
 Gully to near the Lucknow. <A few feet beneath this is the ‘ First Bed of Slate’—a bed 
 of black graphitic shale about 20 feet thick. The Hibernian and Homeward Bound 
 Reefs were worked in this bed, and rich but patchy deposits of gold were obtained. 
 About 150 feet below this is the ‘Second Bed of Slate,’ about 15 feet thick, which has 
 been worked in the Bristol and London Claims. Between these two beds are altered 
 greenish greywackes, one of which is an altered volcanic ash. It is made up of anumber 
 of angular particles in a fine matrix. There is also a peculiar grit or fine conglomerate, 
 made up almost entirely of rounded and flattened particles of about the size of peas. 
 Below the Second Bed of Slate is a hard crystalline ‘ greenstone’ of a similar character, 
 and occupying the same position as on Gympie; then below are altered greenish 
 chloritic rocks, with an amygdaloidal voleanic rock (amygdaloidal diabase). At a depth 
 of 580 feet below the Second Bed is the fine laminated greenish-grey greywacke, with 
 which is associated the black shale known as the ‘ Third Bed of Slate,’ precisely similar 
 to that met with in the Elen Harkins, &e. Good gold was got in the Chatsworth Reef 
 in this bed close to the surface, and the London shaft was in it from 631 feet to near the 
 bottom (736 feet), when they passed into green chloritic rocks again. On comparing 
 this section with that from the Railway Station to Channon-street Bridge, their close 
 agreement will be noticed. The Two-Mile can without hesitation be pronounced an 
 actual continuation of the Gympie auriferous belt. 
 
 “The Two-Mile is situated some distance further away to the west than it would 
 have been had the Gympie Beds continued without any disturbance. The large fault, 
 however, which occurs between the two places has brought about, on a still Jarger scale, 
 a repetition of what has taken place between the Smithfield and Phoenix Claims. The 
 fault shifts the outerop of the limestone and other rocks to the west for a distance of 
 nearly 70 chains, which, allowing for a dip of about 1 in 8 to the east, gives a downthrow 
 to the north of about 1,200 feet. 
 
 “The gold in the reefs at the Two-Mile is in rich patches, and not so continuous 
 as on Gympie. This may be owing to the country, which is reported to be much 
 
 * Mr. Rands uses the term ‘‘Gympie Beds” in the restricted sense of the auriferous strata of the 
 Central District, Gympie, 
 

 
 83 
 
 broken or disturbed by small faults. Rich gold was obtained from the London, 
 Bristol, German, Homeward Bound, Hibernia, and Chatsworth Reefs in the ‘ First and 
 Second Beds of Slate.’ 
 
 “The outcrop of the beds underlying the limestone seems gradually to disappear 
 to the north; thus the outcrop of the ‘Third Bed of Slate’ is at a much less distance 
 west of that of the limestone at the Chatsworth than at the London, while beyond the 
 Chatsworth I have been unable to trace the beds at all. Their absence might be due 
 either to the thinning-out of the beds towards the north, or to a ‘strike-fault,’ the 
 downthrow of which increases towards the north, the effect of which would be the 
 sinking of the intermediate strata below the surface. The thickness of the strata is so 
 great that it is scarcely possible they would have thinned out to nothing in so short a 
 distance, and I think, therefore, that the latter explanation is the more probable. 
 
 “ About five miles north-west of Gympie, in the old Timber Reserve, deposits of 
 stibnite (sulphide of antimony) have lately been discovered in the limestone. Specimens 
 of the fossil Protoretepora occur with its fine markings beautifully picked out in 
 stibnite. Martinia glabra* and Productus brachytherus + are also very numerous. 
 
 ‘““The country for some miles, both east and west of the auriferous rock of 
 Gympie, consists chiefly of laminated grey shales, with interbedded fine-grained sand- 
 stones. These shales are bounded on the west by hardened silicated or jasperised 
 sandstones, beyond which, again, are the granite and serpentine ranges of Kilkivan and 
 the Black Snake. On the north and east they are bounded by the coal-bearing beds of 
 the Tiaro district. The general dip of the shales is east or north-east. In places 
 they dip to the south. At Tamaree there is a bed of white crystalline limestone, from 
 which I obtained a few fossils, among which were Aviculopecten, Spirifera, and 
 erinoid stems. The limestone is being quarried and burnt for use in the Yengarie 
 Sugar Refinery. 
 
 “In several places the shales are covered with a coarse sandstone or freestone 
 beionging to the Desert Sandstone formation. The shales are intersected here and 
 there by dykes and sheets of diorite and sheets of porphyry. 
 
 “Reefs have been worked in several places in the outside shales, but, so far, 
 without much success; some of the crushings have been good, but the cost of carting 
 the quartz in to Gympie has been a great handicap.” 
 
 I have quoted from Mr. Rands’ Report at great length, with the object of 
 recording data for the future comparison of strata of like age in other districts. 
 
 The following is Mr. Etheridge’s list of the fossils which have been obtained 
 from the type district of Gympie itself :— 
 
 Cordaites australis, McCoy ? 
 
 Stenopora gimpiensis, Eth. fil. 
 
 Fenestella fossula, Lonsd. 
 oe sp. ind. 
 
 Polypora? Smithii, Eth. fil. 
 
 Protoretepora ampla, Lonsd. 
 
 Rhombopora ? laxa, Eth. 
 
 Spirifera vespertilio, G. B. Sby. 
 
 Bs trigonalis, var. acuta, Eth. 
 . dubia, Eth. 
 Ps Stokesit, Konig. 
 
 . Strzeleckii, De Kon. 
 
 * Not included in my Colleague’s list. 
 + Not included in my Colleague’s Gympie list, but included in his lists of fossils from Encrinite 
 Creek, Fenestella Hill, Stanwell, Kariboe Creek, and Yarrol = Gympie Beds. 
 
84: 
 
 Martinia (Martinopsis ?) subradiata, G. B. Sby. 
 Strophomena rhomboidalis, var. analoga, Phill. 
 Productus cora, D’Orb. 
 Aviculopecten limeformis, Morris ? 
 
 - ? imbricatus, Eth. 
 
 re multiradiatus, Eth. 
 Mytilops ? sp.ind., Pl. 14, £. 20. 
 Astartella ? rhomboidea, Eth. fil. 
 Cypricardella Jackii, Eth. fil. 
 Conocardium australe, McCoy. 
 Chenomya Etheridgei, De Kon. ? 
 Edmondia ? obovata, Eth. fil. 
 Sanguinolites concentricus, Eth. 
 Pleurotomaria carinata, J. De C. Sby.? 
 Conularia tenuistriata, McCoy. 
 
 e sp. ind. 
 
 Orthoceras, sp. 
 Goniatites, sp. ind. 
 
 Mr. Rands further mentions having discovered in the Upper Limestone bed in 
 the North Smithfield Shaft ‘“‘a specimen of an ‘Ichthyodorulite’ or fin-spine of a fish, 
 belonging probably to the genus Ctenacanthus of the order Placotdei (Agassiz), sub- 
 order Cestraphort” . . . . and adds, “I have since found another specimen of the 
 above in shales in the Deep Creek.” 
 
 MINES IN CONNECTION WITH THE GYMPIE FORMATION IN THE TYPE 
 DISTRICT. 
 GYMPIE GOLD FIELD. 
 
 Among the goldfields of the Colony, Gympie ranks after Charters Towers and 
 Mount Morgan. The field having already been described in considerable detail in this 
 Chapter, it is only necessary in this place to give the following table. Exhaustive details 
 will be found in Mr. Rands’ First and Second Reports * on the Field. 
 
 YIELD OF GYMPIE GOLD FIELD. 
 
 
 
 
 
 
 
 
 
 REEF GOLD. Pe 
 Year. eh aid age es Total Gold. Remarks. 
 Crushed. therefrom. 
 Tons. Oz. Oz. Oz. 
 
 1867 to |) 54d. 9142 1Deduced from figures in Report 
 1875 5 Pt is : of Department of Mines for 
 1876 i, Be er 36,232 1884, p. 11. 
 1877 19,331 43,854: 366 43,854. 
 1878 22,358 40,320 1,244° 41,564 * Includes pyrites, tailings, and 
 1879 26,383 36,799 1,6548 38,453 alluvial. 
 1880 22,562 39,511 3,561 43,072 
 1881 380,066 65,654 2,2078 67,861 3 Includes pyrites, tailings, and 
 1882 44,720 50,162 1504 50,312 alluvial. (?) 
 1883 56,980 © 64,818 Nil 64,818 
 1884 62,085 112,051 Nil 112,051 * Alluvial only. (?) 
 1885 84,146 86,832 2,700 89,532 
 1886 103,946 88,450 150° 88,600 | ® Pyrites, &. 
 1887 90,673 96,940 5,2098 102,149 
 1888 111,962 106,885 2343 107,119 | ® Pyrites, &c. (?) 
 1889 108,317 115,450 1408 115,590 
 1896 101,831 78,044; 3228 78,366 
 
 Total ... re 1,624,487 
 
 * Brisbane; by Authority : 1891, 
 

 
 85 
 NEERDIEK ANTIMONY MINE. 
 
 The history of this mine, which apparently is rich in sulphide of antimony, has 
 been varied by periods of prosperity and depression according to the rise or fall in the 
 price of the metal. The total amount of ore produced from 1873 to 1886 was 930 tons, 
 valued at £11,769. The statistics, however, give the amount of ore raised except in 
 the year 1881, when only the amount shipped is given. 
 
 YIELD oF NEERDIE ANTIMONY MINE. 
 
 
 
 Year. Tons of Ore. Value. 
 £& 
 1873 s0C ane ware cae 15 500 157 
 1874 Sah oe aa Ae 207 sib 2,141 
 1875 ae see ee Se 60 Apr 360 
 1876 Be one ies are 18 ah 216 
 1877 Sun sex: sah see 101 aie 606 
 1878 oa wee re aan 27 e 405 
 1879 fon 0 Ses ane 4, 5010 40 
 1880 aGe aes Ar ast Nil 5100 a00 
 1881 we ane See no 163 ves 1,965 
 1882 ree mY oe .. (No return) bis 
 1883 ea ak AA vale 127 ae 2,550 
 1884 Ac ABC aA “08 198 a 2,969 
 1885 pe <r sae ... (No return) : wee 
 1886 ASa J8C sc ves 110 ae 400 
 Totals... “ 1,080 vais £11,809 
 
 The following description of the mine is taken from a Report by Mr. Rands on 
 the Tiaro District,* which may be referred to for further details. 
 
 “The mine is situated about twelve miles west of Gunalda Railway Station, in 
 the Gympie Shales, south of the Coal Measures. The lodes are in the same series of 
 shales as the Exhibition, Enterprise, and Veteran Reefs—the thick masses of shales 
 which overlie the auriferous beds of Gympie. 
 
 “The Neerdie Antimony Mine has been worked, on and off, since the year 1873. 
 The Neerdie Antimony Company—the original owners—worked it from 1873 to 1876; 
 they did not make it pay. Then a man named Ahrenfeldt leased it on tribute from 
 1876 to 1878, but did very little with it. In 1881 it was leased on tribute to Mr. 
 H. E. King, as managing director of the Wide Bay Antimony and Smelting Company. 
 This company, I am informed, did well by sending ore home direct, even at its low 
 price at that time. They then put up furnaces and flues, and liquated the ore, sending 
 it home as ‘crude antimony,’ which is merely the sulphide of antimony obtained by a 
 process of liquation ; the portion that would not liquate was oxidised and caught in the 
 flues. They did not, however, obtain so high a price for the ‘crude antimony’ as they 
 were getting for the ore; and this, together with a lawsuit with the original company, 
 as to whether the liquated sulphide was smelted antimony or not—they having to pay a 
 higher tribute for smelted antimony—drove the company into liquidation in 1888. The 
 mine was then idle until 1886, when it was sold on conditions to the Neerdie Antimony 
 and Smelting Company. It was worked by this company until the early part of this 
 year. They took outa large quantity of good ore, but the expenses of the furnaces 
 and liquation, and the low price of antimony at the time, caused them also to go into 
 liquidation, the mine being thrown on the hands of the original owners again. 
 
 
 
 * The Coal Measures, Neerdie Antimony Mine, and Teebar and Culgoa Copper Lodes. Brisbane: 
 by Authority : 1890, 
 
86 
 
 “So far as I am able to gather from information supplied to me, about 1,139 
 tons of ore and ‘crude antimony’ have been sold from the mine. Of this about 250 
 tons of ore, won by the original company and by Mr. Ahrenfeldt, fetched a little over 
 £10 per ton. The Wide Bay Antimony and Smelting Company and the Neerdie 
 Antimony and Smelting Company sold 890 tons of ore and ‘crude antimony,’ at 
 prices varying from £8 15s. per ton to £17 10s. per ton. 
 
 “The New South Wales returns for the ten years 1872 to 1881, show that in 
 that colony 1,072 tons of antimony (metal, ore, and regulus; the proportions of each 
 are not given) sold for £28,616, or an average of £26 13s. 9d. per ton. At the present 
 time the price of antimony is higher than it has been for a long time. Quotations in 
 the American Mining Journal are :— 
 
 26th July, 1889—Star regulus ... se ... £61 to £63 per ton. 
 Crude antimony a oo GR Ge ET. oy, 
 50 per cent. ore tk ; LS 20 
 
 “ The ore from the mine is of a good quality and can be ‘picked’ up to between 
 50 per cent. and 60 per cent. At the present prices it should pay to work if there 
 is as good ore in the bottom level as there was in the upper ones. 
 
 ‘Up to the present work has been carried on on one lode only, and on but one 
 ‘shoot’ in that lode. There has not been sufficient prospecting for fresh ‘shoots,’ nor 
 have the other lodes that are known to exist been sufficiently tried.” 
 
—— ————“— -  — = 
 
 
 
 CHAPTER VIII. 
 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 THE GYMPIE FORMATION OUTSIDE OF THE TYPH DISTRICT, 
 
 IncLtupING YARROL, Mount Biag@enDEN, GreBANGLE, Mount SHAMROCK, HEIDSVOLD, Canta, RAGLAN, 
 LANGMORN, CALLIOPE, Koorncat, RockHAMPTON, DEE AND Don Rivers, St. LAWRENCE. 
 
 Mineral Areas—viz., Kilkivan and Black Snake, Kilkivan Mercury Mines and Mount Coora 
 Copper Mine, Gayndah Gold Fields, Mount Biggenden, Gebangle and Mount Shamrock 
 Gold Fields, Brovinia Gold Field, Paradise Gold Field, Raglan, Calliope, Norton, Cania 
 and Kroombit Gold Fields, Rockhampton Gold Fields (excluding Mount Morgan), Yatton 
 Gold Field, Gooroomjam Diggings, Warwick Gold Fields. 
 
 SepaARATED from the Gympie District by the granitic ranges which extend from 
 Kilkivan to the heads of Munna Creek, and the granitic mass of Boolboonda, are some 
 strata from which Mr. Rands has obtained fossils which enable us to place them on the 
 horizon of the Gympie Beds.* Among these strata beds of limestone and sandstone 
 close to Yarrol Station have yielded Productus brachytherus, G. Sby., P. sp. ind. (a), 
 Pl. 18, £. 6, and Pleurophorus Randsi, Eth. fil., as determined by my Colleague. Mr. 
 Rands also mentions the following :—Fenestella, Retepora, Ceriopora, Spirifera (two 
 species), Strophomena rhomboidalis, and another species, Rhynchonella, Aviculopecten, 
 Pleurotomaria, Mourlonia Strzeleckiana, Morris, and Orthoceras. 
 
 A galena lode, in slate country probably of the same age, has been worked about 
 a mile and a-half south of Yarrol Station. : 
 
 Near the Bismuth and Gold Mine of Mount Biggenden are limestones and 
 siliceous slates, the latter predominating. The limestone has been metamorphosed and 
 has become crystalline. ‘ From the foot of the spur leading up to the mines (about 10 
 chains) the rock consists entirely of siliceous slates, which dip very steeply to the north- 
 west. Above the mine is a bed of limestone about 70 feet in thickness, and above that 
 again the slates occur, together with an altered sedimentary rock containing quartz, 
 felspar, hornblende, and olivine. Rocks of the same character occur on the ridge north- 
 east of the gully and right away on to Mount Biggenden itself. The Mount Biggenden 
 deposit consists of an irregular mass of magnetite, somewhat semicircular in shape, 
 bounded on the north by the slates and on the south by the limestone.’’+ 
 
 Limestones, conglomerates, and slates form the country-rock of the Mount 
 Hastings Gold Mine, which is situated on the south side of Biggenden Creek, about 
 two miles south-east of the Mount Biggenden Mine.t 
 
 Gebangle, six miles north-north-west of Mount Shamrock, is situated in a 
 country-rock consisting chiefly of stratified mud-rocks and siliceous slates, having a 
 
 
 
 ; * Report by W. H. Rands on the Goldfields of Raglan, Calliope, &c. Brisbane: by Authority : 1885, 
 p. 10. 
 + Report by W. H. Rands on Mount Biggenden Bismuth Mine, &c. Brisbane: by Authority : 1890, 
 
 cf 0s Cit. Ds os 
 
88 
 
 general dip of 50° to N. 15° E.* The stratified rocks of Mount Biggenden, Mount 
 Hastings, and Gebangle probably belong to the Gympie Beds, although there is no 
 paleontological evidence nearer than Yarrol in support of this view. 
 
 The Mount Shamrock Gold, Silver, and Bismuth Mines, near the junction of 
 Didcot and Chowey Creeks, are situated in a series of massive slates, hardened siliceous 
 and felspathic sandstones, quartzites and conglomerates, traversed by igneous dykes. 
 These stratified rocks have undergone sufficient metamorphism to render it difficult to 
 distinguish the direction of either their dip or strike.t They probably belong to the 
 Gympie Beds. 
 
 Between Eidsvold Township and Lochaber Station, “about a mile from Lochaber, 
 one passes on to fine-grained sandstones, quartzites and slates, which are dipping 
 20° to the S. I should refer this formation, on lithological grounds, to the Devonian, 
 which covers so large an area of this district; the same beds are met with along the 
 road from Mount Perry to Eidsvold, where occasional beds of limestone occur.”{ The 
 Lochaber rocks, as well as those between Mount Perry and Hidsvold, are now classed 
 with the Gympie Beds. 
 
 The country-rock of the Cania Gold Field “ consists of alternating layers of 
 sandstone, slates, and limestones. The latter are of a pisolitie structure, and are in 
 parts fossiliferous. I obtained, after a long search, a few specimens from a bed of lime- 
 stone about 3 miles up the Three-moon Creek from the diggings. They were not, 
 however, in a very good state of preservation. . . . . In the creek just opposite to 
 the township, the formation is dipping 80° to E.15°S.” At Kariboe Creek, on Kroombit 
 Diggings, west of Cania, similar strata have also yielded some fossils. The whole are 
 referred to the Gympie Beds. The fossils from Cania and Kariboe Creek, as determined 
 by my Colleague, are :— 
 
 Spirifera bicarinata, Eth. fil. 
 Martinia ? productoides, Eth. fil. 
 Martiniopsis ? subradiata, var. Morrisit, Eth. fil. 
 Athyris ambigua, J. de C. Sby. 
 »  Landsi, Eth. fil. 
 Rhynchonella, sp. ind. 
 Orthis resupinata, Martin. 
 Productus brachytherus, G. Sby. 
 
 a semireticulatus, Martin ? 
 Lingula mytiloides, J. Sby. ? 
 Modiomorpha ? Daintreei, Eth. fil. 
 Goniatites, sp. ind., Pl. 15, figs. 14, 15. 
 
 In addition to the above Mr. Rands mentions the occurrence of corals. 
 
 The country-rock of the Raglan Gold Field (south of the mouth of 
 the Fitzroy) consists chiefly of argillaceous and siliceous slates and hardened 
 sandstones or quartzites. These beds strike north and south, and are on the 
 whole nearly vertical, although at times they have a slight dip to the west. Their 
 strike is from north to south. At Mount Holly a thick bed of conglomerate 
 occurs. About a mile to the east of the Reserve is a bed of blue encrinital and 
 coralline limestone dipping at a high angle to the west. This limestone is full 
 of encrinite remains. Another bed of limestone two miles to the east runs 
 
 * Loc. cit., p. 4. 
 
 + Report by W. H. Rands on the Gold and Silver Deposits in the Neighbourhood of Mount Shamrock. 
 Brisbane: by Authority : 1886. 
 
 + Report by W. H. Rands on the Hidsvold Gold Field. Brisbane: by Authority: 1887, 
 

 
 89 
 
 almost at right angles to the Mount Holly bed. At its western extremity for two 
 or three miles it is full of encrinite stems. It is intersected by a north-westerly dyke 
 of porphyry. 
 
 From a limestone on a hill near Langmorn, and about six miles to the south-west 
 of the above, Mr. Rands obtained some specimens of Pelecypods. A similar limestone 
 forms what are known as the Bald Hills. Several auriferous reefs and a copper lode 
 occur among the slates of this neighbourhood.* 
 
 In addition to the fossils collected by Mr. Rands, the late Mr. James Smith made 
 a considerable collection from the Raglan and Langmorn Limestones. Mr. Smith 
 identified the limestones, without hesitation, with those of Dalma and Lilymere near 
 Rockhampton, and the slates in connection with the Raglan and Langmorn Limestones 
 with the slates of the Rockhampton District. Mr. Smith obtained from a deposit of 
 stalagma at Langmorn, which there, as at Dalma, represents caves from which the 
 surrounding limestone has been denuded, a large bone which is as yet undetermined. I 
 have no difficulty in classing the Raglan + and Langmorn Beds with the Gympie Beds. 
 They have yielded the following fossils as determined by Mr. Etheridge :— Favosites, sp. 
 ind. ; Cyathophyllum, sp. ind., Pl. 7, fig. 1; and Myriolithes ? queenslandensis, Eth. fil.f 
 
 A bed of marble, probably the equivalent of some of the limestone beds at 
 Langmorn and Raglan, crosses the Calliope River about a mile below Carrara Station. 
 It “forms a bar across the river in a north-north-westerly direction, and has been 
 quarried and shipped in small schooners which at high tide can come up the river as far 
 as this bar. This marble would be valuable for statuary purposes. At the crossing 
 [of the Rockhampton and Gladstone road] is a dyke of porphyry, with small blebs of 
 quartz, running parallel with the marble. This has partially decomposed into kaolin. 
 
 “The limestone is met with every here and there on either side of Brennan’s 
 Flat, on Sheep Station Hill, Ten Men’s Gully, Gordon’s Gully, and other places [on 
 the Calliope Gold Field] ; then going in the same direction, and. crossing the watershed 
 on either side of New Zealand Gully and on to the Boyne River at the settlement 
 called Marblestone, where it occupies nearly the whole area between Raggote Creek 
 and the river. At Marblestone it isin places a greyish-white marble, which will take 
 a good polish. It again occurs on the south side of the Boyne. I was unable to detect 
 any organic remains in these limestones; they have become very crystalline, and in all 
 probability any fossils they may have contained have been destroyed during their change.” § 
 Several auriferous reefs occur in slates and schists associated with the limestones. 
 
 At Kooingal extensive deposits of limestone have been successfully exploited 
 for fossils by the late Mr. James Smith. The fossils prove the limestones to be approxi- 
 mately of the age of the Gympie Beds. So far as they have been determined by my 
 Colleague they are as follow :— 
 
 Monticulipora, sp ind., Pl. 38, figs. 1, 2. 
 Stenopora, sp. ind., Pl. 6, figs. 14, 15. 
 Crinoid stems. 
 
 Fenestella, sp. ind. 
 
 Aviculopecten multiradiatus, Eth. 
 
 * Report by W. H. Rands on the Goldfields of Raglan, &c. Brisbane: by Authority: 1885. 
 
 +I regret to say I cannot concur with my Colleague in the classification ofthe Raglan Limestone 
 with the Gympie Beds. The fossils that I have seen from Raglan, including in a later collection made by 
 Mr. Smith Cystiphyllum, remind me far more of those of the Burdekin Beds. I have never seen Mavosites 
 from the Gympie Beds, and certainly not Cystiphyllum ; neither have I observed any trace of Ayriolithes 
 from Raglan. (2... junr.) 
 
 + Occurs also in the Lilymere and Dalma Limestones, near Rockhampton ( fide Smith). 
 
 § Report by W. H. Rands on the Gold Fields of Raglan, Calliope, &c., 1885, p. 3. 
 
90 
 
 From the neighbourhood of Rockhampton, chiefly owing to the labours of Mr. 
 C. W. de Vis and the late Mr. James Smith, we have obtained a rich collection of 
 fossils, which not only enables us to place the strata of that district on the horizon of 
 the Gympie Beds but also to add considerably to the Gympie list. 
 
 After collecting from the limestones at Dalma and Lilymere, Mr. Smith came 
 to the conclusion that in the Rockhampton District the greater part of the fossiliferous 
 beds, including the “ Annelid”’ beds of Thozet’s Creek, the Trilobite beds of Crow’s 
 Nest, the Encrinite and Fenestella bearing beds of Fenestella Hill, the Encrinite and 
 Productus Beds of Encrinite Creek, near Mount Morgan, and the Fenestella and Pro- 
 ductus bearing beds of Lake’s Creek and the Training Wall Quarries, lie unconformably 
 on what he calls the “ Central Queensland Shales,” of which the strata seen in the 
 Rockhampton quarry may be taken as the type, and of which the Lilymere and Dalma 
 limestones form a part. He remarked on “the extreme paucity of fossils in the old 
 shales, their different composition, the high angles at which they li, their uniform dip 
 and strike, and their thick accumulations ; whereas the fossiliferous rocks are generally 
 thin, lie at all low angles, and dip and strike in every direction.”’ As has already been. 
 noted, Mr. Smith identified the Dalma and Lilymere Limestones with those of Raglan 
 and Langmorn. In the latter district he admitted that the limestone beds are infer- 
 stratified with and conformable to the “ Central Queensland Shales’ (an observation 
 entirely in accord with Mr. Rands’ description of the Raglan District), so that the 
 unconformability at Rockhampton, if it exists, must be a local and unimportant one. 
 
 In the above remarks it must be noted that the fossiliferous beds of Stewart’s 
 Creek, Wycarbah, Rosewood, and Stanwell (in part) are not included. 
 
 The Rockhampton District has not yet been geologically mapped, and I have only 
 Mr. Smith’s notes and a few hasty traverses of my own to refer to. 
 
 An immense series of limestone beds is developed on both sides of the Fitzroy 
 River, from Rockhampton to near Yaamba. The limestone beds crop out over a tract 
 of country about ten miles in width, as measured across the strike, which is almost 
 always to the north-west. On the south-western side are the limestones of Mount 
 Siluria, west of the Lower Gracemere Lagoon, and Lion Creek. These limestones, so 
 far as I know, have yielded no fossils. A peculiar structure brought out by the 
 weathering of the Mount Siluria Limestone, and supposed at one time to point to a 
 coralline origin, proved on microscopic examination to be merely oolitic or concretionary. 
 Some hard, greenish, fine-grained siliceous and calcareous sandstones, associated with 
 the limestone, yield, however, abundant encrinite stems. This limestone and the 
 associated strata dip at high angles to the south-west. Limestones in the same line of 
 strike are seen crossing Limestone Creek, which falls into the right bank of the Fitzroy, 
 from three to four miles above its junction with Black Gin Creek. Limestone beds are 
 also seen striking to the north-west from the south end of Lilymere Lagoon. The 
 strike of these beds, if produced to the south-east, would pass through the Murray 
 Lagoon, about a mile north-east of which is the Rockhampton Quarry, in beds 
 of hardened sandstones and shales, dipping to N.E. at 70°. These strata have 
 yielded some undistinguishable plant-impressions. Between the quarry and Murray 
 Lagoon are the comparatively soft grey sandstones and shales which form the gentle 
 elevation known as the Athelstane Range. The “ Rocks” above the Suspension Bridge 
 consist of hardened or jasperised slates, &c., which dip N.N.W. at 30°. On the left 
 bank of the Fitzroy from nearly opposite the mouth of Lion Creek, limestone beds are 
 traceable almost continuously north-westward for at least a mile or two north of 
 the Long Island in the Fitzroy. Interealated with the limestones near Ramsay’s 
 Creek, Belmore Creek, and the Long Island, are hardened slaty rocks and hardened 
 

 
 31 
 
 fine-grained quartzose greywackes. On the left bank of the river, opposite the north 
 end of the Long Island, the strata dip at 45° to N.E., while opposite the south end of 
 the Island they dip at 70° to S.W. In the whole of the region above described the 
 frequent reversals of dip probably bring about frequent repetitions, at the surface, of 
 the various limestone and other beds. 
 
 In what is no doubt a prolongation of the Dalma Limestones, near Mount Etna, 
 about four miles east of Yaamba, are the famous Olsen’s and Johansen’s Caves, which 
 are alluded to in another place. . The Dalma Limestone contains masses of stalagma, 
 with vertebrate remains, attesting the former existence of caverns in the limestone. 
 
 East of the Fitzroy, the low hills at the foot of Berserker Range show sand- 
 stones and shales dipping to the south-west ; so that there is probably a synclinal trough 
 between these hills and the Rockhampton quarry. In Thozet’s Creek, which falls into 
 the left bank of the Fitzroy, below the reserve for pasturage, hard flinty fine-grained 
 siliceous sandstone dips at an angle of 80° to W. This sandstone is a mass of infilled 
 tubes, believed by many to be made by Annelids.* Fragments of a similar rock are 
 found lying loose on the Athelstane Range, on the ridges at Gracemere, and at Kabra. 
 I should be inclined to think that the ‘ Annelid Bed” dips beneath the limestone seen 
 on Limestone Creek to the north-west, although Mr. Smith regarded it as lying uncon- 
 formably on the latter. 
 
 In Lake’s Creek and the “ Training Wall Quarries,’ on the left bank of the 
 Fitzroy below the mouth of Lake’s Creek, are fine-grained dark-greenish sandstones 
 full of Fenestella, Protoretepora, Brachiopods, &c., probably slightly below the horizon 
 of the Thozet’s Creek Beds. The quarries have recently yielded to the late Mr. James 
 Smith specimens of Lepidodendron, probably LZ. australe, and Calamites, sp. ind. In the 
 Cawarral District the strata graduate from serpentinous slates and schists to serpentine 
 (auriferous). The originally sedimentary origin of the Cawarral Serpentine, however 
 metamorphosed, is evidenced by the occurrence of. a specimen, collected by Mr. Smith, 
 and now in the Geological Survey Collection, containing the impression of a small fossil, 
 which my Colleague says ‘‘may be either a perforate Spirifera or Athyris.” 
 
 Grits and slates are seen in the Berserker Ranges, and on the road from Rock- 
 hampton to Cawarral. These beds may be beneath the horizon of the Lake’s Creek Beds. 
 
 At Taranganba, south of Yeppoon, is a considerable mass of flaggy quartzite beds, 
 striking for the most part north and south, and on the whole vertical, although some- 
 times contorted. The quartzites invariably contain a good deal of fine pyrites, in which 
 traces of gold are obtainable. The quartzites are traversed by many leaders, reefs, and 
 lodes, which are in some degree auriferous. They are also intersected by dykes of 
 acidic felstone.t 
 
 North Keppel Island, in Keppel Bay, opposite Yeppoon, is composed of slates 
 and greywackes dipping at high angles to the north-west, and intersected by dolerite 
 dykes. 
 
 South-west of Rockhampton, Stony Creek, near Stanwell, brings down boulders 
 of pale-green fine-grained hardened siliceous sandstone, rich in the remains of Trilobites, 
 Encrinites, and Brachiopods. The strata from which these boulders have been derived 
 are seen in situ at Crow’s Nest, near Mount Morgan. 
 
 Neerkol Creek, near Stanwell, has also yielded to Mr. Smith a large collection of 
 fossils of the genera Spirifera, Productus, Strophomena, Orthis, Aviculopecten, and 
 Fenestella. 
 
 
 
 * See my Colleague’s remarks in the Monograph of the Silurian Fossils of Girvan, Fasc. 3, p. 304. 
 Mr. Etheridge doubts the Annelid origin of the Thozet’s Creek burrows. 
 + See Report by R. L. Jack on Taranganba Gold Mine. Brisbane: by Authority : 1889, 
 
92 
 
 On the opposite side of the range (which is capped by Desert Sandstone), similar 
 strata at Fenestella Hill and Encrinite Creek, near Mount Morgan, on the Dee Fall, 
 have yielded to Mr. Smith a profusion of similar fossils. 
 
 The locality of the Don River from which the Rev. W. B. Clarke obtained the 
 fossils described in 1872 by Mr. R. Etheridge, F.R.S.,* is somewhat doubtful, but as the 
 Don River near Bowen cannot possibly be the locality in question, it is probable that 
 the Don River referred to is that which falls into the Dee in Lat. 24° S. 
 
 Mr. De Vis’ fossils from the “ Rockhampton District” are said by Mr. De Vis 
 to come “from the Agricultural Reserve—from the Fitzroy at Laurel Bank, about ten 
 miles from Rockhampton, westwards to the Nine-mile Lagoon; thence to the Corpora- 
 tion Quarry, Athelstane Range, and to the northern outcrop (at foot of Berserker’s) of 
 the synclinal beneath the township and bed of river.’’ The district thus described is 
 probably altogether fairly within the Rockhampton Beds, as the term is used by us. 
 
 The following are lists of the fossils from the various localities in the Rock- 
 hampton District, as determined by my Colleague. They sufficiently justify our 
 uniting the Rockhampton Beds with the Gympie Formation. 
 
 (1) Litymere Limestone. 
 
 Myriolithes ? queenslandensis, Eth. fil. Mourlonia Strzeleckiana, Mor. 
 
 Retzia ? lilymerensis, Eth. fil. 
 
 (2) Laxe’s Creek anp Training Walt QUARRIES. 
 
 Calamites, sp. ind. 
 Lepidodendron australe, McCoy ? 
 Fenestella fossula, Lonsd. 
 Martinia? productoides, Eth. fil. 
 
 Productus cora, D’Orb. 
 
 + subquadratus, Mor. 
 Goniatites planorbiformis, Eth. fil. 
 
 i sp. ind., Pl. 15, figs. 14, 15. 
 
 (3) Buackrettow’s Dicernas. 
 
 Fenestella fossula, Lonsd. 
 Polypora ? Smithii, Eth. fil. 
 
 Protoretepora ampla, Lonsd. 
 
 (4) Srony Creek (STANWELL) AND Crow’s Nest. 
 
 Poteriocrinus ? Smithii, Eth. fil. 
 Arms of crinoid, Pl, 7, fig. 7. 
 
 > Pla7 gre: 
 Crinoid stems. 
 Granatocrinus ? Wachsmuthii, Eth. fil. 
 Phillipsia Woodwardi, Eth. fil. 
 
 : ? sp. ind. 
 
 Griffithides seminifera, Phill. 
 Rhombopora ? laxa, Eth. 
 Spirifera vespertilio, G. B. Sby. 
 
 + trigonalis, var. crassa, De Kon. 
 
 $3 bicarinata, Eth. fil. 
 Martinia? productoides, ©th. fil. 
 Athyris Roysit, Levéillé. 
 Rthynchonella pleurodon, Phill. 
 Orthis resupinata, Martin. 
 
 
 
 Orthis australis, McCoy. 
 Productus cora, D’ Orb. 
 
 »  brachytherus, G. Sby. 
 
 »  undatus, Defrance. 
 
 a semireticulatus, Martin ? 
 
 3 ~ sp. tnd, (6), PI12 digr is. 
 
 » sp. ind. (c), Pl. 18, fig. 4. 
 Chonetes cracowensis, Eth. 
 
 es sp. ind. (a), Pl. 18, fig. 10; PI. 
 37, figs. 21, 22. 
 
 7 sp. ind. (6), Pl. 18, figs. 7, 8, 18. 
 Aviculopecten Laurenti, Eth. fil. 
 Loxonema, sp. 
 
 Euomphalus, sp. 
 Platyschisma oculus, J. de C. Sby. 
 Bellerophon stanvellensis, Eth. fil. 
 
 * Quart. Journ, Geol, Soc, Lond., xxviii., p. 333 et seq. 
 
—_— = 
 
 | 
 
 
 
 (5) EncrinitE Creek. 
 
 Poteriocrinus crassus, Miller? 
 
 Productus brachytherus, G. Sby. 
 
 (6) Fenestetia Hirt. 
 
 Poteriocrinus crassus, Miller ? 
 Fenestella internata, Lonsd. 
 
 Polypora? Smithii, Eth. fil. 
 Productus brachytherus, G. Sby. 
 
 (7) ATHELSTANE RANGE. 
 
 Crinoid stems. 
 Orthis resupinata, Martin. 
 
 Chonetes cracowensis, Eth. 
 
 i sp. ind. (b), Pl. 18, figs. 7, 8, 13. 
 
 (S) Don River.* 
 
 Phillipsia dubia, Eth. 
 Spirifera, sp. ind. (a), Pl. 9, fig. 12. 
 Productus longispinus, J. Sby.? 
 
 Naticopsis ? harpeformis, Eth. 
 Murchisonia carinata, Eth. 
 
 (9) “ Rocxnampron Districr’’ (Dr Vis). 
 
 Lasiocladia ? Hindei, Eth. fil. 
 Cladochonus tenuicollis, McCoy. 
 Zaphrentis profunda, Eth. fil. 
 Actinocrinus, sp. ind., Pl. 7, fig. 9. 
 Cup of crinoid, Pl. 44, fig. 7. 
 Impressions of crinoid calix, Pl. 44, fig. 8. 
 Mesoblastus ? australis, Eth. fil. 
 Tricelocrinus ? Carpenteri, Eth. fil. 
 Archeocidaris, sp. 
 Griffithides seminifera, Phill. 
 Glauconome, sp. ind., Pl. 44, fig. 11. 
 Dielasma sacculus, var. hastata, J. de C. 
 Sow. 
 
 af ? sp. ind., Pl. 40, figs. 1, 2. 
 Spirifera, sp. ind, (a.), Pl. 9, fig. 12. 
 
 * trigonalis, Martin. 
 
 aS pinguis, J. Sby. 
 Reticularia lineata, Martin ? 
 Orthis australis, McCoy. . 
 Strophomena rhomboidalis, var. analoga, 
 
 Phill. 
 
 Productus, sp. ind. (d.), Pl. 40, fig. 4. 
 Aviculopecten Laurenti, Eth. fil. 
 Pterinopecten Devisit, Eth. fil. 
 Mytilops ? corrugata, Eth. fil. 
 Parallelodon costellata, McCoy. 
 Nucula, sp. ind., Pl. 40, fig. 10. 
 Platyschisma rotundata, Eth. 
 Yvania Konincki, Eth. fil. 
 Luciella? Graye, Eth. fil. 
 Murchisonia, sp. a. 
 
 As sp. b. 
 
 + Sp. 0s 
 Bucania textilis, De Kon. 
 Porcellia Pearsi, Eth. fil. 
 Nautilus, sp. 
 
 55 ? ammonitiformis, Eth. fil. 
 
 Orthoceras, sp. 
 Gyroceras dubius, Eth. fil. 
 Goniatites planorbiformis, Eth. fil. 
 Deltodus ? australis, Eth. fil. 
 
 The Rockhampton District as a whole has afforded the following fossils :— 
 
 Oalamites, sp. ind. 
 
 Lepidodendron australe, McCoy ? 
 Lasiocladia ? Hindei, Eth. fil. 
 Oladochonus tenuicollis, McCoy. 
 Zaphrentis profunda, Eth. fil. 
 Actinocrinus, sp. ind., Pl. 7, fig. 9. 
 Cup of crinoid, Pl. 44, fig. 7. 
 
 
 
 Arms of erinoid, Pl. 7, fig. 7. 
 es A: Pie ys ue. 8. 
 Stems of erinoid. 
 Impressions of crinoid calix, Pl. 44, fig. 8. 
 Poteriocrinus ? Smithii, Eth. fil. 
 ¥ erassus, Miller ? 
 Mesoblastus ? australis, Eth. fil. 
 
 
 
 * See remarks on p. 92. 
 
94 
 
 RookHAMPTON District Fossits—continued. 
 
 
 
 Granatocrinus ? Wachsmuthii, Eth. fil. Productus semireticulatus, Martin ? 
 Tricelocrinus ? Carpenteri, Eth. fil. a longispinus, J. Sby. 
 Archeocidaris, sp. sp. ind. (b.); P1212, fig, 15: 
 Phillipsia dubia, Eth. % sp. ind. (c.), Pl. 18, fig. 4. 
 
 : Woodwardi, Kth. fil. sp. ind. (d.), Pl. 40, fig. 4. 
 
 “h ? sp. ind. Chonetes cracowensis, Eth. 
 Griffithides seminifera, Phill. a sp. ind. (a:),-Fl.. la, aig ales 
 Fenestella fossula, Lousd. Pl. 87, figs. 21, 22. 
 
 “ internata, Lonsd. S sp. ind, (b.), Pl. 18, figs. 7, 8, 18. 
 
 4s sp. ind. Aviculopecten Laurenti, Eth. fil. 
 Polypora ? Smithit, Eth. fil. Pterinopecten Devisii, Eth. fil. 
 Protoretepora ampla, Lousd. Mytilops ? corrugata, Eth. fil. 
 Glauconome, sp. ind., Pl. 44, fig. 11. Parallelodon costellata, McCoy. 
 Rhombopora ? laxa, Eth. Nucula, sp. ind., Pl. 40, fig. 10. 
 Myriolithes ? queenslandensis, Eth. fil. Naticopsis ? harpeformis, Eth. 
 Dielasma sacculus, var. hastata, J. de C. Loxonema, sp. 
 
 Sby. Euomphalus, sp. 
 
 Dielasma? sp. ind., Pl. 40, figs. 1, 2. Platyschisma oculus, J. de OC. Sby. 
 Spirifera, sp. ind. (a.), Pl. 9, fig. 12. _ rotundata, Eth. 
 
 ke vespertilio, G. B. Sby. Mourlonia Strzeleckiana, Mor. 
 
 = trigonalis, Martin. Yvania Konincki, Eth. fil. 
 
 a trigonalis, var. crassa, De Kon. Luciella ? Graye, Eth. fil. 
 
 < pinguis, J. Sby. Murchisonia carinata, Eth. 
 
 a bicarinata, Eth. fil. Pi Sp. a. 
 Reticularia lineata, Martin ? ' sp. 0. 
 Martinia ? productoides, Eth. fil. * Sp. ¢. 
 Retzia ? lilymerensis, Eth. fil. Bellerophon stanvellensis, Eth. fil. 
 Athyris Roysii, Leveillé. Bucania textilis, De Kon. 
 Ethynchonella pleurodon, Phill. Poreellia Pearsi, Eth. fil. 
 Orthis resupinata, Martin. Nautilus, sp. 
 
 » australis, McCoy. - ? ammonitiformis, Eth. fil. 
 
 Strophomena rhomboidalis, var. analoga, Orthoceras, sp. 
 
 Phill. Gyroceras dubius, Eth. fil. 
 Productus cora, D’Orb. Goniatites planorbiformis, Eth. fil. 
 
 Be brachytherus, G. Sby. i sp. ind., Pl. 15, figs. 14, 15. 
 
 _ subquadratus, Morris. Deltodus ? australis, Eth. fil. 
 
 + undatus, Defrance. 
 
 
 
 Of the above, Fenestella fossula, Polypora ? Smithii, Protoretepora ampla, 
 Fehombopora ? laxa, Spirifera vespertilio, Spirifera trigonalis, Strophomena rhomboid- 
 alis, var. analoga, Productus cora, and Orthoceras, sp., are common to the Gympie 
 Beds of the type district. Spirifera bicarinatx, Martinia ? productoides, Orthis 
 resupinata, Productus brachytherus, P. semireticulatus, and Goniatites, sp. ind. (Pl. 
 15, figs. 14, 15), are common to the Cania Beds. Productus brachytherus and Mour- 
 lonia Strzeleckiana are common to the Yarrol Beds. Myriolithes ? queenslandensis 
 . common to the Langmorn Beds. Productus subquadratus is common to the Yatton 
 
 eds. 
 
 A scrubby hilltop, three miles south-west of the Yatton Gold Field Township 
 (west of the mouth of the Styx River), is capped by a bed of grey limestone which dips 
 
—=  _— — __—S—-~—>=s rarer 
 
 
 
 95 
 
 S.S.E. at 45°, but owing to the thickness of the scrub and other difficulties the relation 
 of the limestone to other rocks in the neighbourhood is not ascertainable. This 
 limestone has yielded a large number of fossils in good preservation, amongst which 
 my Colleague has recognised :— 
 Spirifera lata, McCoy. 
 _ Stokesit (common to Gympie). 
 Martinia Darwinit. 
 Productus subgquadratus (common to Rockhampton Beds). 
 “ sp. ind. (f.), Pl. 44, fig. 18. 
 Aviculopecten limeformis (? common to Gympie Beds). 
 Eurydesma, sp. ind. 
 
 Between Yatton and St. Lawrence, in ascending the coast range from Waverley 
 Station to Killarney by the old road from St. Lawrence to Peak Downs, a great thick- 
 ness of coarse green conglomerate is exposed. The sandy matrix and the boulders are 
 of similar material—namely, felsite and porphyrite—so that the conglomerate does not 
 weather in the customary manner of conglomerates. The exposed surfaces, on the 
 contrary, show the pebbles shorn off down to the same level as the matrix, so that it is 
 only on a fresh fracture that the true character of the rock can be seen. In this respect 
 the conglomerate resembles the Gympie conglomerate. It probably belongs to the same 
 formation as the Yatton Limestone. 
 
 Mr. Smith found his ‘“ Central Queensland Shales’? (Rockhampton Beds) 
 unconformably overlaid by the strata of the Styx River Coal Field (Burrum Beds) on 
 Barrack Creek, a tributary of the Styx. Between the Styx Coal Field and the Bald Hills 
 he observed among the Central Queensland Shales a thick bed of encrinital limestone, 
 striking north-north-west, and very probably a continuation of the Dalma and Rock- 
 hampton Limestones. 
 
 I have little hesitation in mapping the greater part of the district lying between 
 the Burrum Coal Field on the east, and the Dawson River Coal Field on the west, from 
 Gayndah on the south to Broadsound on the north, as of the age of the Gympie Beds. 
 This area, it may be mentioned, was mapped as Devonian in the Geological Map of 
 Queensland issued in 1886. In some districts within this large area the Gympie Beds 
 are overlaid by Basalt, Desert Sandstone, the Burrum Beds, and by the Middle and 
 perhaps the Upper Series of the Bowen River Coal Field, while on the other hand 
 granite and other plutonic and intrusive rocks and masses of serpentine occupy portions 
 of the area. 
 
 The late Mr. Daintree observed, at Mount Wyatt Diggings, certain slates and 
 shales containing Ohonetes sarcinulata, an Orthis allied to O. rustica, Receptaculites, and 
 Leptena, as determined by Sir F. McCoy. These rocks were unconformably over- 
 laid by beds, probably of the ‘Star’ Series, containing Lepidodendron. On the strength 
 of the fossils the strata first alluded to were assumed to be of Upper Silurian age. The 
 assumption was based on a single distiuctly specifically determined Brachiopod, Chonetes 
 sarcinulata, now known to range upward into Devonian times, an Orthis, which might be 
 allied to an Upper Silurian species, without being itself of that age—the genus ranging 
 all through the Silurian, Devonian, and Carboniferous—a Receptaculites* and a Leptena 
 (Silurian and Devonian) not specifically determined. I have not been able to identify 
 the locality referred to by Mr. Daintree, but as I observed both the Star Beds and the 
 Gympie Beds in the neighbourhood, I think it probable that the Chonetes, &c., beds 
 belong to the latter. 
 
 * Every effort has been made, both in London and Brisbane, to trace this fossil but without success. 
 (RE, junr.) 
 
96 
 
 Treating the Gympie Beds from Lat. 21° southward as a whole, and including all 
 the fossiliferous rocks of the Rockhampton District, Kooingal, Cania, Yatton, Yarrol, 
 Raglan, and Langmorn, we have a very extensive list of fossils. By reference to 
 the lists given on pages 43 and 92-94, several points of interest may be noted. 
 
 It will be seen, in the first place, that there is a very decided hiatus between the life 
 of the Gympie Formation and that of the Devonian, not a single species being common 
 to the two formations, and only three genera of Actinozoa, viz., Favosites, Pachypora, 
 and Oyathophyllum, and two of Brachiopoda, viz., Spirifera and Rhynchonella. 
 
 Turning to the other members of the Permo-Carboniferous System, we find that 
 all the genera of Plants, viz., Calamites, Lepidodendron, and Cordaites, known in the 
 Gympie Formation, are also present in the Star Formation. Among Crinoids, Actino- 
 crinus, and among Crustaceans, Phillipsia, are common to both. Among Polyzoa, 
 Fenestella is present in both. Lastly, the two formations have no less than nine genera 
 of Mollusca in common—viz., Spirifera, Reticularia, Retzia, Rhynchonella, Orthis, 
 Strophomena, Chonetes, Naticopsis, and Porcellia. None of the genera of plants found in 
 the Gympie Formation are met with either in the Middle or Upper Bowen Formations. 
 Of Actinozoa, Stenopora is the only genus common to the Gympie and Middle Bowen. 
 Of Polyzoa, Fenestella and Protoretepora are genera common to the Gympie and 
 Middle Bowen. Of Mollusca, fourteen genera are common to the Gympie and Middle 
 Bowen—viz., Dielasma, Spirifera, Martiniopsis, Productus, Chonetes, Aviculopecten, 
 Modiomorpha, Astartella, Chenomya, Mourlonia, Bellerophon, Porcellia, Orthoceras, and 
 Goniatites. Productus and Goniatites are genera common to the Gympie and Upper 
 Bowen. 
 
 No less than ninety-five species are peculiar to the Gympie Beds. Twelve are 
 common to the Star Beds, seventeen to the Middle Series of the Bowen River Coal Field, 
 and two to the Upper Series. It would appear from this that the Gympie Beds have 
 most in common with the Middle Bowen River Beds, and nearly as much with the Star 
 Beds. It must be recollected, however, that the Bowen River Beds and the Star Beds, 
 especially the latter, have as yet been but imperfectly collected from. 
 
 It will be remembered that Lepidodendron has never yet been traced upward into 
 the Bowen River Beds, although it is a characteristic plant of the Star Beds. It has, 
 however, been found in the Gympie Beds in the Training Wall Quarries at Rockhamp- 
 ton, and naturally forms a strong link connecting the Star and Gympie Beds. The 
 . abundance (in individuals) of Encrinites and Trilobites is another point which the 
 Gympie and Star Beds have in common. Several species of Spirifera, Rhynchonella, 
 Orthis, Strophomena, and Chonetes, and some of Gasteropoda, are also common to the 
 Star and Gympie Beds. 
 
 On the other hand, Fenestella is very abundant both in the Gympie Beds and 
 the Middle Bowen River Beds. Three species of Spirifera, one of Reticularia, one of 
 Martinia, one of Orthis, one of Strophomena, three of Productus, one of Chonetes, one 
 of Aviculopecten, one of Chenomya, one of Platyschisma, one of Bellerophon, one of 
 Porcellia, and one of Orthoceras are common to the Gympie and Middle Bowen Beds. 
 
 In the face of the greater number of species common to the Gympie and Middle 
 Bowen Beds than are common to the Gympie and Star Beds, it is not without some 
 misgivings that I come to the conclusion that the Gympie Beds come nearer to the Star 
 than to the Middle Bowen Beds. I was indeed till recently inclined to favour the idea 
 that the auriferous Gympie Beds were only the coal-bearing Middle Bowen Beds some- 
 what metamorphosed, and the presence of beds of graphite among the Gympie rocks 
 lent colour to this view. But now, on the completion of my Colleague’s work, it strikes 
 me forcibly that if the two series were identical there could not be such a large number 
 

 
 97 
 
 of species in the one which are not represented in the other. The Gympie Beds 
 contain ninety-five species peculiar to themselves, and the Middle Bowen Series 
 thirty-four species peculiar to itself. I am quite open to conviction should future 
 evidence turn up to prove the identity of the Gympie Beds either with the Star 
 or Middle Bowen Beds; but in the meantime I think it safer to keep the Gympie 
 Beds apart and to assign to them a position beneath the Star Beds, for the reasons 
 already stated. 
 
 Iam not able to identify the Gympie Formation with anything in New South 
 Wales or Victoria, unless mere lithological resemblance can be taken as a guide; but, 
 considering how near to the southern border of Queensland the Gympie Formation has 
 been traced, it is more than likely that some of the New South Wales sedimentary rocks, 
 at present doubtfully referred to Silurian and Devonian, may yet prove to be on the 
 Gympie horizon.* 
 
 The Star Beds have undergone, so far as I have observed, no very great degree 
 of metamorphism. Portions of them, such as the Drummond Beds, may be said to have 
 undergone no metamorphism at all. The Gympie Beds, on the other hand, are at least 
 in places considerably metamorphosed. 
 
 The Lower Series of the Bowen River Coal Field, which is believed to be newer 
 than the Gympie Beds, has suffered in the Mackay District a very considerable amount 
 of metamorphism. 
 
 MINES IN CONNECTION. WITH THE GYMPIE FORMATION OUTSIDE OF 
 THE TYPE DISTRICT. 
 
 KILKIVAN AND BLACK SNAKE. 
 
 “Most of the work at Kilkivan has been the driving of tunnels in a sheet of 
 white porphyry, which occurs in the face of a range running north and south. The 
 porphyry varies greatly in thickness. There are no defined reefs at all in the porphyry, 
 but only minute veins of quartz with oxides of iron and manganese. Where the man- 
 ganese dioxide occurs the veins are the richest in gold. In some parts of the porphyry 
 these veins are very numerous, and the veins are very patchy. Where these patches 
 occur, however, the whole of the mass will pay to crush. No large quantity of stone 
 can be obtained. Two men who have been working in the Long Tunnel P.C., which 
 is considered the best claim in the porphyry, after six months’ work, have just had a 
 crushing of 8} tons for 24 oz. of smelted gold. The cost of carting and crushing alone 
 was £3 per ton. 
 
 “The country around Kilkivan consists entirely of metamorphic rocks, such 
 as serpentine, hornblendic and micaceous schists. All the reefs found in this 
 district occur in these rocks. From the Rise and Shine Reef very good specimens 
 of gold in the quartz were obtained in the upper part. Lower down the stone 
 changes to a mundic consisting greatly of zinc-blende with some iron pyrites and a 
 little galena. 
 
 “The country between Kilkivan and the Black Snake and Mount Coora is 
 entirely of schists—chiefly hornblendic—and mica-schists, which have a steep inclina- 
 tion to the north-west. 
 
 “The gold-bearing reefs of the Black Snake district occur in a micaceous 
 porphyrite. This rock consists of a felsitic base with porphyritic crystals of oligoclase 
 
 * T suspect that the Gympie Beds will prove to be identical with the New South Wales strata termed 
 by me ‘‘ Carboniferous”’—formerly known as ‘‘ Lower Carboniferous”—so largely represented in the Port 
 Stephens District. Possibly the Star Beds will also be identical. (R.Z. unr.) 
 
 G 
 
98 
 
 felgpar and Mieg, some pyrites, and here and there viridite and chlorite from the 
 decomposition of some of the original constituents of the rock. This rock occupies 
 a small area of about 3 square miles. The reefs generally have a north-west 
 bearing and are perpendicular, or have a slight underlie to the east or south- 
 east. The ores from these reefs are complex; in the Mariner’s Reef, for instance, 
 at a small depth the ore consists of iron, copper, arsenical pyrites, silver-lead ore 
 (galena), and a small amount of sulphide of antimony. The gold in this ore was equal 
 to a little over 1 oz. per ton, the silver to about 25 oz. per ton. Copper, as carbonate 
 or sulphide, is met with, sometimes sufficiently rich to smelt; 50 tons from the 
 Rose, Shamrock, and Thistle Reef were sold to the Mount Coora Copper Mining 
 Company. 
 
 “Outside this area of porphyrite, northward towards Mount Coora, are altered 
 rocks consisting of serpentine and of an altered volcanic rock, probably an altered 
 dolerite. The whole area was most probably of the same volcanic rocks, parts of which 
 have undergone a greater change. It is in these rocks that the Mount Coora and 
 Mount Clara copper lodes oceur. 
 
 “The Black Snake is now almost entirely deserted. This state of affairs 
 is due, in my opinion, not so much to the poverty of the reefs, as to the fact that 
 the land, having become private property, is closed to general enterprise. This 
 field has, moreover, got a bad name owing to the investment of a large amount of 
 capital in erecting furnaces and extravagant crushing plants instead of in the mines 
 themselves.” * 
 
 In his “Report on the Geology and Mineral Resources of the Districts of Kilkivan 
 and the Black Snake,’ + Mr. Rands describes the Rise and Shine (which has given 
 2,760 oz. of gold from 1,336 tons of stone), Morning Star, Welcome, Perseverance, and 
 New Year’s Reefs at Kilkivan, and the Rose, Shamrock, and Thistle, Tableland, New 
 Zealand, Black Snake, Homeward Bound, Mariner’s, and Victoria Reefs at Black Snake. 
 Of the Black Snake Reefs, Mr. Rands observes: “ Judging from specimens of ore I saw, 
 and also from assays of samples, there can be no doubt as to the high value of the ores 
 in this district, and as the reefs generally are of a good average width, some of them, at 
 any rate, should pay well to work. The ore would require special and expensive treat- 
 ment to extract the gold and other metals of commercial value, and it would probably be 
 found advisable to merely concentrate them on the field and send them elsewhere for 
 treatment.” 
 
 Important copper lodes occur in the Black Snake District at Mount Coora and 
 Mount Clara and other locatities, but are not now worked 
 
 KILKIVAN MERCURY MINES AND MOUNT COORA COBALT MINE. 
 
 Mr. Rands reported as follows on the Queensland and Woif Cinnabar Lodes at 
 the end of 1886 :— 
 
 “The matrix of the lodes consists of quartz and calcite. Both lodes are looking 
 well, showing cinnabar all through the stone. 
 
 “ At the Queensland Lode the shaft is down 42 feet. The lode runs north and 
 south. At the bottom of the shaft the lode is divided into two parts by a ‘ horse’ of 
 mullock. On the eastern or foot wall is a small vein of quartz which is very rich in ore; 
 next to this is about 8 inches of quartz and calcite with ore throughout it, while on 
 the hanging-wall is another mass of vein-stuff containing cinnabar. A little to the 
 
 
 
 * W. H. Rands, in Report of Department of Mines for 1885, 
 + Brisbane: by Authority : 1886, 
 

 
 
 
 99 
 
 north of the shaft the lode takes a sharp bend to the west. The country is an altered 
 conglomerate or agglomerate, probably of volcanic origin, as it is full of angular 
 particles, 
 
 “On the Wolf Lode a level has been driven on the bank of the gully for 170 
 feet on the lode. The country for the first 100 feet or so consists of sandstone and 
 shale dipping south-west at this point, and above them is a volcanic ash, much decom- 
 posed, and containing often large angular pebbles. The lode runs north-east, and 
 averages about 1 foot in thickness. The matrix contains much more calcite than that 
 of the Queensland Lode. 
 
 “ A cross-cut lower down the gully cuts several lodes or veins. At 19 feet, one of 
 1 foot in thickness of calcite; at 55 feet, a lode of 1 foot 2 inches wide showing good 
 ore ; at 119 feet is a vein of calcite which appears to be dipping towards some leaders 
 at 145 feet, which contains cinnabar; and at 200 feet the Wolf is cut 4 feet 2 inches 
 wide, and contains a very good percentage of cinnabar. 
 
 “Very rich pieces of nearly pure cinnabar have been picked up in a gully on 
 this claim, supposed to have come from a small vein a short distance from the Wolf 
 Claim. 
 
 “So far as the work has at present gone the prospect for the future of these 
 mines looks very encouraging.’’* 
 
 Nothing is recorded of the output of the cinnabar mines. In 1877 the Warden 
 reported that ‘considerable progress has been made by the Messrs. Hester at their 
 cinnabar works. They have for some time past kept the machines at Gympie fully 
 supplied with quicksilver. The quicksilver supplied by Hester Brothers is preferred by 
 the amalgamators at Gympie to the best article of its kind imported.” Very little 
 progress has been made, although it was reported in 1886 that a company had been 
 formed to work them. 
 
 Recently information has come to hand that a valuable deposit of stream 
 cinnabar has been discovered. 
 
 Several cinnabar lodes occur in the district on the heads of Wide Bay Creek. 
 
 A cobalt lode occurs in a spur of Mount Coora, consisting of serpentine. The 
 lode has been traced over half-a-mile north and south, and underlies to the west at 
 about 50°. ‘“ At its outerop the lode consists of 10 or 12 feet of a talcose casing, with 
 cobalt ore throughout it next to the foot-wall ; then 22 feet of cobalt ore with a brown 
 siliceous matrix (this forms the chief ore-bearing portion of the lode); above this again, 
 next to the hanging-wall, is a mineral similar to pimelite, consisting of silicates of 
 magnesia and alumina with a little silicate of nickel. A tunnel, 80 feet in length, has 
 been put in on the back of the lode, and from the end of the tunnel a cross-cut. has been 
 driven through the lode, which passed through 15 feet of the main portion or cobalt- 
 bearing part of the lode, and then about 10 feet of the casing seen at the surface; 
 beyond this another mass of cobalt ore occurs, the width of which has not yet been 
 ascertained. The ore is that known as earthy cobalt, consisting of oxides of cobalt, 
 manganese, iron, and a little copper. 
 
 “‘ Assays have shown the average ore to contain about 6 per cent. of cobalt, which, 
 according to last Sydney quotations, is worth about £13 10s. per ton. By hand-picking 
 the ore it might be brought up to about 10 per cent., which would be worth £23 per 
 ton. The extent of the lode, and the large body of ore it contains, makes this 
 undoubtedly a very valuable and important discovery.” + 
 
 
 
 * Report of the Department of Mines for 1886. 
 + W. H, Rands in Report of the Department of Mines for 1886, 
 
100 
 
 GAYNDAH GOLD FIELDS. 
 
 MOUNT SHAMROCK. 
 
 This goldfield is a comparatively new field, and its output appears for the first 
 time in 1877, as 3,348 oz. of gold from 3,151 tons of stone crushed. In the same year 
 5 tons of bismuth ore were exported. 
 
 Mount Shamrock is a low hill about 145 feet in height above the level of Didcot 
 Creek, which runs at its foot on the eastern side. The hill consists almost entirely of a 
 dark-coloured massive slate, which is intersected by dykes of porphyry. It was on 
 the summit of this hill, close to where their shaft now is, that the prospectors first 
 discovered the gold in a piece of iron-stained stone lying at the surface. 
 
 Mount SHamrock Prospecting Cram. 
 
 Ina shaft 30 feet deep “the following materials were passed through, in the 
 order mentioned, in layers, all of which were dipping away steeply to the east :— 
 
 “J. A breccia consisting of angular fragments of a fine-grained aluminous and 
 siliceous rock, cemented together with a hard cement of oxide of iron and silica, 
 throughout which are numerous blebs of quartz. 
 
 “2. A yellow ochre containing a fair percentage of oxide of bismuth. 
 
 “3. A brown iron ochre with veins of crystallised glassy quartz running 
 through it. 
 
 “These ochres form the principal part of what has been passed through in the 
 shaft. The two together must be at least 8 feet to 10 feet in width, and they contain 
 numerous veins and bunches of oxide of bismuth. 
 
 “4, Earthy red hematite, with siliceous veins containing also broken particles 
 and blebs of glassy quartz. 
 
 “ All these materials contain gold in considerable quantity, the gold in some 
 places being beautifully crystallised. 
 
 “Much doubt has been expressed as to the nature of this deposit. Both from 
 the character of the stone and the regular manner in which it strikes and dips, I 
 am of opinion that it is a lode, the breccia being formed by the breaking up and 
 subsequent cementing together of particles of the walls and matrix of the lode. 
 The fissure in which the lode is formed appears to have acted as the channel for 
 the passage of water of hot springs to the surface, for all the materials, the 
 crystallised gold, the hard siliceous and iron cement of the breccia, and the ochreous 
 materials are such as would have only been formed by deposition from solution 
 in water. 
 
 “The gold appears to be especially associated with the bismuth, for the veins of 
 oxide of bismuth are exceptionally rich. A small sample of the oxide assayed by 
 Mr. Hamilton contained 62 per cent. of metallic bismuth and 252 oz. of gold per ton of 
 the material. 
 
 “A dyke of white felspar-porphyry can be traced down the hill from a point 
 immediately south of the shaft in a west-north-west direction. It is very probable that 
 this dyke may have influenced the richness of the lode at this point. 
 
 “Tn No. 1 and No. 2 North small quantities of gold have been found associated 
 with the porphyry dyke. 
 
 “Mount Melville consists of massive blue slates and hardened sandstones, 
 intersected by dykes of felspar-porphyry of a similar character, and probably a 
 continuation of those met with in the northern part of Mount Shamrock. A 
 

 
 
 
 101 
 
 sample taken from the outcrop yielded gold equal to about 2 oz. 12 dwt. 13 gr. to 
 the ton, but a trial crushing of 31 ewt. yielded only 4 dwt., or a little over 25 dwt. to 
 the ton. 
 
 * At the foot of this hill a small reef is being worked. It is from 2 to 10 inches 
 wide, consisting of quartz with a large percentage of the oxide of iron and manganese. 
 At the bottom of the shaft, in one place, there is a vein, 1 inch wide, consisting almost 
 entirely of pyrolusite (oxide of manganese). An assay from this reef gave 16 dwt. of 
 gold and 6 oz. of silver per ton. It intersects a dyke of porphyry. The foot-wall is of 
 dolerite. 
 
 “ At Mount Ophir is a large reef of white translucent quartz, stained in patches 
 with oxide of iron. It contains a good deal of molybdenite and specks of iron pyrites. 
 At 25 feet a hole was drilled into the reef; the débris obtained from the hole, on being 
 washed, gave a very good prospect indeed. The rock of which this—the northern— 
 side of Mount Ophir consists is made of fine felspathic dust containing small and more 
 or less rounded particles of a micro-crystalline felspathic rock. Fine gold is obtained 
 on crushing and washing pieces of this rock.’’* 
 
 Mr. Rands, in the Report above quoted, gives an account of the Old Chowey 
 Reefs and Stanton-Harcourt alluvial diggings, and of the Allendale, Hannan’s, Union, 
 Lady Mary, and other silver lodes. The argentiferous lead ores are associated with 
 arsenical pyrites and zinc-blende. Mr. Rands observes: “The amount of silver in 
 the lodes, as far as assays have at present shown, is small—only from 30 oz. to 
 40 oz. to the ton, which of itself will not pay to work, especially with a narrow reef. 
 They all contain some gold. In the Allendale, which is the only shaft well into the 
 sulphides, the ore contains as much as 1 oz. of gold to the ton. In 1886, the amount of 
 ore raised was 75 tons, valued at £1,350. In 1887 the return was nil.” 
 
 In a later Report,t Mr. Rands says:—‘‘ The deposit has been worked down to a 
 depth of 215 feet, in the shape of a large square shaft about 40 feet across. This shaft 
 was perpendicular down to a depth of 140 feet, from which point it inclines to S. 
 at 40°, and to E. at 7°. 
 
 “In my former report on this mine, I said that the deposit was probably in the 
 form of a ‘pipe,’ rather than a lode, and that the metallic minerals, and cementing 
 materials, had probably been deposited from solution in water which has come up through 
 fissures. The work since done bears out this opinion. 
 
 “ For the first 50 feet the stone consisted of a breccia of fine-grained aluminous 
 and siliceous rocks cemented together with a hard cement of oxide of iron and silica, a 
 yellow ochre containing a fair percentage of oxide of bismuth, a brown iron ochre, and 
 earthy red hematite with siliceous veins through it ; and carbonate of bismuth in small 
 pockets. 
 
 “ At 50 feet in depth there was a large cavity filled in with a siliceous sinter, so 
 light that it would float in water. Numerous such cavities, but smaller in size, have 
 been met with at various depths. 
 
 ‘‘A tunnel has been driven into the deposit from the eastern slope of the hill, at 
 a depth of 56 feet from the summit. This tunnel was in slates and stratified mud-rock, 
 to a point 100 feet from the shaft, when the wall forming the boundary of the deposit 
 occurs running W. 40° N. Prospects of gold can be got in this 100 feet, and it, or a 
 part of it, will probably be worked at some future time. 
 
 
 
 * Report on the Gold and Silver Deposits in the Neighbourhood of Mount Shamrock. By W. H. 
 Rands. Brisbane: by Authority : 1886, 
 
 + On the Mount Biggenden Bismuth Mine, Gebangle, and the Mount Shamrock Mine. Brisbane; 
 by Authority : 1890, 
 
102 
 
 “There are numerous boulders of decomposed porphyry in the centre of the 
 deposit at this level. On the western side of the deposit there is a dyke of kaolinite 
 formed from decomposed porphyry; it is running north and south, and it is per- 
 pendicular. 
 
 “Slates are met with on the western side of this dyke, dipping north-north-east. 
 There is a small vein of molybdenite very rich in gold in these slates. 
 
 “As the width of the working place is about 30 feet, the width of the whole 
 deposit from east to west is about 140 feet at this level. 
 
 “ Below the 50-feet level sulphurets began to appear, and there was comparatively 
 little free gold to what was obtained near the surface. At 70 feet in depth the ore 
 contained a great amount of iron pyrites. 
 
 - “At 100 feet in depth a second tunnel has been driven into the hill to cut the 
 deposit. Slates and mud-rock occur in this tunnel from the mouth to a point 78 feet 
 from the main workings, when the wall forming the eastern boundary of the deposit is 
 met with again, running W.N.W., and dipping 8.S.W. at 70°. The deposit in the 
 tunnel is in layers dipping to E. at 25°. Prospects of gold can be obtained throughout 
 it, especially when the pyrites is in any quantity. The character of the stone in the 
 portion being worked is much the same from this level down to the present depth—215 
 feet. 
 
 “Jt consists of fragmentary mud-rock, with a soft greyish tufaceous material, 
 interlaced with veins and fissures, filled with sulphides of bismuth and iron, molybdenite, 
 arsenical pyrites, quartz, ime, &c. There are some beautiful specimens of molybdenite 
 with sulphide of bismuth imbedded in it. Tetradymite—a telluride and sulphide of 
 bismuth—occurs in small quantities in association with quartz. Small cavities occur in 
 the deposit all the way down; these are often lined with well-crystallised minerals, 
 among which I may mention beautiful needle-shaped crystals of bismuthinite, crystals 
 of quartz, pearl-spar, and calcite. 
 
 “The manager, Mr. Higgings, informed me that the bismuth ore decreases in 
 quantity at a depth. At 140 feet in depth a ‘horse’ or mass of mud-rock comes in on 
 the northern side, and dips S. at about 40°, and from this depth the workings have 
 dipped with it. At the bottom the size of the workings is 35 feet by 33 feet; but this 
 does not represent the whole of the stone to be taken out, as the eastern and southern 
 walls of the workings consist of stone of similar character to that being worked. The 
 layers of the deposit dip away to the east from the ‘horse’ of mud-rock. There are 
 large detached masses of a hard, very fine-grained rock at this level—one was so 
 large that it was thought the deposit had cut out.” . . . “<A twenty-head 
 battery is kept continually going, and up to the present time 11,864 tons have been 
 crushed for a yield of 6,416 oz. 11 dwt. of gold, or an average of 10 dwt. 5 gr. of gold 
 per ton. 
 
 “Tailings, estimated at 8,000 tons, from the crushings down to the 150-feet 
 level, have been stacked. These are estimated to contain about 1} oz. of gold per ton.” 
 
 MOUNT BIGGENDEN. 
 
 This remarkable deposit of gold and bismuth is described by Mr. Rands* as 
 follows :— 
 
 “The workings are on a spur running up in a south-easterly direction to Mount 
 Biggenden itself. The spur lies between one of the heads of the Two-mile Creek on 
 the west, and a gully on the north-east. 
 
 * Report on Mount Biggenden Bismuth Mine, &c. Brisbane: by Authority: 1890, 
 

 
 ' 
 
 
 
 103 
 
 “The high ridges to the west of the Two-mile Creek are of granite. The granite 
 bends round to the east about a quarter of a mile up the creek, and crossing the creek, 
 forms the range that divides the Two-mile Creek waters from those of Biggenden or 
 Degilbo Creek. 
 
 “From the foot of the spur up to the mine, a distance of about 10 chains, 
 the rock consists entirely of siliceous slates, which dip very steeply to the north- 
 west. Above the mine is a bed of limestone about 70 feet in thickness, and 
 above that again the slates occur, together with an altered sedimentary rock, con- 
 taining quartz, felspar, hornblende, and olivine. Rocks of the same character 
 occur on the ridge north-east of the gully, and right away on to Mount Biggenden 
 itself. 
 
 “The Mount Biggenden deposit consists of an irregular mass of magnetite, 
 somewhat semicircular in shape, bounded on the north by the slates and on the south 
 by the bed of limestone. 
 
 “The following is a description of the deposits and workings :— 
 
 “ Cutting No. 1 has been driven into the spur in a southerly direction for a 
 distance of 95 feet. The cutting is situated at the top of an inclined tramway, which 
 runs down the hill to the Two-mile Creek. 
 
 “The first 12 feet of the cutting is in a light-grey soil with a few boulders of a 
 fine-grained felspathic rock in it. The next 12 feet is of hard altered rock containing 
 the minerals schorl, chlorite, and olivine. Then comes 6 feet of « decomposed dioritiec 
 rock, which has decomposed in concentric rings around kernels of the undecom- 
 posed rock. Next to this there is 9 feet of decomposed granite, and then 7 feet of 
 a soft white kaolinite. From this point to the face of the cutting, which is 35 feet 
 in height, is a mass of magnetite, lying in more or less horizontal layers. Near the 
 surface, above the magnetite, there is a siliceous rock containing a large amount of 
 arsenical pyrites. 
 
 “The magnetite contains numerous cavities, the sides of which are generally lined 
 with well-formed octahedral crystals of that mineral; some of these cavities are filled 
 in with calcite, while others are Jined with decomposed radiating prismatic crystals, 
 which I believe were originally hornblende. 
 
 “In and around the calcite there are also cavities containing a black powder 
 consisting chiefly of the binoxide of manganese. The oxide of manganese is generally 
 rich in oxide and carbonate of bismuth. 
 
 “At the end of the cutting in the western corner there is a mass of this calcite 
 of about 15 feet in length and 3 feet in height, in which some fine specimens of 
 bismuthinite (sulphide of bismuth) have been obtained. 
 
 “The magnetite contains a little bismuth throughout it. <A large amount of ore 
 has been taken and stacked for treatment from this cutting, but owing to the difficulty 
 of concentrating it up to a sufficiently high percentage of bismuth, it has not been sent 
 away. The difficuity lies in the separation of the oxides and carbonates of bismuth 
 from the magnetite, as their specific gravities are so much alike; the average specific 
 gravity of the oxide of bismuth being 4°38, carbonate of bismuth 6°5, and that of 
 magnetite 5°2. 
 
 “ After washing a dishful of this ore as carefully as possible, 700 out of 900 parts 
 of the concentrates were of magnetite, and could be extracted with a magnet. This 
 cutting was not being worked. 
 
 “No. 2 Cutting is situated about 100 feet south-east of the mouth of No. 1, on 
 the eastern fall of the spur, and at 15 feet higher level than No. 1. 
 
104 
 
 “The ridge is much steeper on the eastern than on the western fall. The bed 
 of limestone is 70 feet south of this cutting. It is an open quarry, with a face 80 feet 
 in width and 22 feet in height. 
 
 “In the face of this quarry there is a large mass of crystallized calcite, 11 feet 
 in height from the floor and 27 feet in width. Magnetite occurs on either side of this 
 calcite, which appears to have filled a large cavity. 
 
 “There are numerous pipe-shaped and circular cavities; these, and all the joints, 
 are filled with a fine dust, consisting chiefly of black oxide of manganese and a little 
 cobalt, from which fact this working place has received the name of the ‘cobalt cutting.’ 
 The percentage of cobalt is very small. Dr. March, of Maryborough, gives two analyses 
 of this black dust :— 
 
 
 
 Bismuth ... a wt as me sds we 44°45 
 Cobalt... ee Sas fee PP = va tee 
 Nickel ... Sih hs at ce ae ano 
 Iron sae ay sine FEC Sa ie we 13°65 
 Manganese — ne ast was a hp OO 
 Lime and magnesia _.... ea ‘a0 oe! ae a. 
 Riliez as. sas ne = ie ne sr. 0:90 
 
 100°00 
 
 “Of a second sample he says—‘It consists of black oxide of manganese with 
 5°97 per cent. of cobaltic oxide.’ Messrs. Johnson and Matthey return only 2 per cent. 
 of cobalt. The first sample was exceptionally rich in bismuth. 
 
 “Native bismuth, the oxide and carbonate of bismuth, and at times a 
 little sulphide of bismuth, occur in this dust. The native bismuth is generally 
 adhering to the calcite, and is often in the form of ‘casts’ of the rhombohedral 
 crystals of calcite, showing that it must have been deposited there subsequently to 
 the calcite. 
 
 “Four pieces of native bismuth were found in a small cavity, weighing together 
 36 lb.; small pieces up to 4 or 5 oz. in weight are continually being obtained. 
 
 “Small crystals of aragonite often encrust the calcite of these pipes. Some of 
 these pipes are 2 or 3 feet in diameter and several feet in length. 
 
 “During my visit oxide of manganese was found coated with the mineral 
 erythrine—a hydrated arsenide of cobalt. This mineral is of a peach-blossom colour, 
 and reniform in shape. At present it has only been found in small quantities; when 
 found in quantity it is very valuable for the manufacture of ‘smalt’—a blue pigment. 
 I believe this is the only occurrence of this mineral known of in Queensland. 
 
 “ Around the calcite is a layer of soft material rich in bismuth ore, and above 
 this layer is a quartzose rock containing arsenical pyrites and specks of metallic 
 bismuth. This rock will require crushing machinery to extract the bismuth if found in 
 sufficient quantities. Near the mouth of the cutting is some jasperized quartzose rock. 
 
 ‘No. 3 Cutting—known as the gold cutting—is on the western slope of the 
 ridge. It is 105 feet south-west of the face of No. 1 Cutting. It is almost entirely in 
 a soft aluminous rock—probably a decomposed porphyry. Near the face there is a 
 band of decomposed granite, which carries a little gold and dips to the south. A mass 
 of magnetite lies above the aluminous rock. Carbonate of bismuth occurs in this 
 cutting ; it is coloured green with silicate of iron. 
 
 ‘“‘ Gold has been traced along the surface, by means of small pot-holes, between 
 this aud No. 1 Cutting. The prospects, however, are very small, and do not repre- 
 sent more than 2 dwt. to the ton. The manager reports that he has quite lately 
 

 
 105 
 
 obtained bismuth ore, and gold equal to about 4 or 5 dwt. to the ton, in one of these 
 holes, in a decomposed rock containing hornblende. He adds that it is free from 
 magnetite, and will dress-up to 15 per cent. of bismuth, and probably 3 or 4 oz. of 
 gold to the ton. 
 
 “A shaft, 42 feet in depth, has been sunk about 30 feet from No. 1 Cutting. 
 It passed through—first, a decomposed rock with lumps of native bismuth and carbonate 
 of bismuth; next through a siliceous rock containing a large amount of arsenical 
 pyrites ; then through 25 feet of calcite; and lastly through solid magnetite. 
 
 “The plan adopted for concentrating the ore is to first pass it through a half-inch 
 screen; the coarser portion is afterwards hand-picked. All that goes through the 
 screen is carted to a Cornish jigger, and put through with a mesh of 25 holes to the 
 inch. Whatever passes through the jigger is then ‘forked’ in a streaming-box. By 
 this method about 1 ton of concentrates is obtained from 20 tons of dirt. The manager 
 has found streaming to answer much better than sluicing, as much less water is used, 
 and much less of the finer bismuth ore is lost. 
 
 ‘With reference to the origin of the deposit, it is an irregular deposit. Its 
 exact limits are not well defined, as the surface is covered with soil and large boulders of 
 magnetite, which first drew the prospector’s attention to it; but it is somewhat semi- 
 circular in shape. 
 
 “The deposit in question extends but a short distance in any direction; its 
 greatest length is under 400 feet, and its greatest breadth about 150 feet. It certainly 
 is not in the form of a bed. I am of opinion that the iron came up from below in 
 solution, perhaps as hydrated oxide; that it was precipitated as peroxide of iron, and that 
 it was subsequently changed into magnetite—ferrous oxide and sesquioxide of iron—at 
 the time when the surrounding rocks were altered; the calcite and other minerals — 
 viz., the bismuth, manganese, and cobalt ores—being deposited subsequently in the 
 numerous cavities in the magnetite. 
 
 “Tt is difficult, at present, to say much as to the commercial value of the deposit. 
 Jt is being worked as a bismuth mine pure and simple. As far as the workings have at 
 present gone they are mere scratchings on the surface, and the bismuth ores are only 
 taken from the ‘pockets’ or cavities in the magnetite, and several tons of material have 
 to be removed to obtain 1 ton of the ‘ dirt,’ and 20 tons of this have to be concentrated 
 to give 1 ton of ore containing about 10 per cent. of bismuth, worth £5 12s. per unit, or 
 about £55 per ton. Mr. Roberts, the manager, reports that during October about 100 
 tons of dirt have been raised and treated for a yield of rather more than 5 tons of 
 concentrates, averaging 10 per cent. of bismuth. 
 
 “The difficulty of separating the bismuth ore from the magnetite greatly limits 
 the quantity of stone that can be treated.” 
 
 GEBANGLE. 
 
 Several reefs, among which are the Mount Allen, Victoria, Lady Frances, 
 Gebangle, Pride of Gebangle, Lord Nelson, Just-in-Time, Mount Toohey, Morning Star, 
 Homeward Bound, and Grecian Bend, are described by Mr. Rands in his ‘‘ Report on 
 Mount Biggenden, &e.” The field was opened in 1888. The country-rock varies from 
 siliceous slates and greywacke to a “bedded volcanic agglomerate,” granite and 
 
 porpayay: BROVINIA 
 
 The existence of gold in this locality has been known for many years. It was, 
 however, only in 1886 that the reward was claimed for the discovery of payable gold. 
 
106 
 There are five reefs in the May Queen Claim. Ten tons of stone sent to Gympie 
 gave a return of 1 oz. 14 dwt. of gold per ton. Machinery is about to be erected on 
 the field. , 
 
 In 1887, the total yield of gold from the Gayndah fields, which include 
 Mount Shamrock, Gebangle, Chowie Creek, Stanton - Harcourt, River Bend, and 
 Brovinia, is given as 3,348 oz. from 3,151 tons; in 1888, 8,810 oz. from 6,292 tons; 
 in 1889, 1,793 oz. from 3,840 tons; in 1890, 2,791 oz. 
 
 PARADISE GOLD FIELD. 
 
 This new goldfield is situated partly in granite or porphyry country and partly 
 in siliceous slates, which may be assumed to belong to the Gympie Formation. The 
 following description is taken from a Report by Mr. Rands,* who gives, in addition, a 
 minute account of the different reefs. The Paradise and William Tell Reefs are in 
 the “ porphyry” country and the remainder in the slate. 
 
 ‘“‘The Paradise Gold Field is situated on the south side of the Burnett River, 
 about eight miles north-west of Degilbo Station, and about two miles below the mouth 
 of Yarrabil Creek, the creek on which Gebangle is situated. 
 
 “Gold was discovered in reefs here about the middle of the year 1889, by 
 Messrs. Allen and party. In my report on Gebangle, &c., published early in the year 
 1890,¢ I mentioned two reefs as being prospected in this district. Only during the 
 last six or eight months, however, have any number of people been attracted to this 
 field, and during that time fresh reefs have been discovered and prospecting has been 
 going on apace. 
 
 “ At the present time the population of the field is estimated at about 400. 
 
 “The reefs extend back for a distance of two miles from the Burnett River, 
 and are situated on the steep ridges which le between Scrubby or Paradise Creek 
 and Finney’s Creek. The site of the township is on the alluvial flat which fringes 
 the river. 
 
 “ The field at present is not a large one; it covers an area of from one and a-half 
 to two miles in a north-and-south direction, by, say, an average of half-a-mile in an east- 
 and-west direction. Very similar rock, however, extends over a much larger area, so 
 that there is every probability of an extension of the area over which gold-bearing reefs 
 will be found. 
 
 “The country-rock is for the most part a hard dark-coloured siliceous slate, with 
 altered sandstone in places. It is only here and there that the dip of the slates is 
 sufficiently defined to be determined. 
 
 “In the neighbourhood of the Paradise P.C. and Leishman’s William Tell, 
 and crossing the ridge along which the road to Mount Shamrock runs, there is a 
 porphyry with a granitic structure, and consisting of about equal parts of quartz 
 and felspar. The Paradise P.C. shaft has passed through this rock down to its present 
 depth, 130 feet. 
 
 “All the way down Yarrabil Creek, from Gebangle to near its junction with the 
 Burnett, slates and sandstones dip steeply to the north-west. On the north-eastern 
 side of Scrubby or Paradise Creek, near its junction with the river, there are ridges 
 containing thick beds of a white crystallized limestone running in an east-north-easterly 
 
 * Brisbane: by Authority: 1891. 
 + Report on Mount Biggenden Mine, Gebangle, &c. Brisbane: by Authority ; 1890. 
 

 
 
 
 107 
 
 direction. I was unable to detect any organic remains in’this limestone. Nearer 
 the creek there was another bed of similar limestone running in a more northerly 
 direction. 
 
 “The reefs run in various directions, but the majority of them have a more or 
 less easterly and westerly bearing. Most of them are approaching the perpendicular ; 
 the Lady Margaret Reef, which underlies very flatly to the west, is a notable exception. 
 Several of the reefs are small; in many cases they appear to be increasing in size at a 
 depth, and the stone is quite as rich as in the narrower portions of the reef. The latest 
 development in the Paradise P.C.—the deepest shaft on the field, where over 5 feet of 
 quartz in width has been cut through at a depth of 180 feet—speaks well for the 
 prospect of the reefs at a depth. 
 
 “The quartz has generally a faint bluish tint, caused by finely divided pyrites 
 occurring throughout it. It contains also larger specks of pyrites and minute particles 
 of galena and zinc-blende, though these latter minerals are by no means common. The 
 gold exists in a very finely divided condition, and it is not often that it is visible in the 
 quartz. 
 
 ‘““So far as prospecting up to the present has gone, the gold appears to be 
 disseminated very regularly through the reefs, and not to run in ‘shoots’ as is usually 
 the case. 
 
 “The crushings amount in the aggregate to 552 tons, which have yielded 
 1,068 oz. of gold, or a little under 2 oz. of gold to the ton—an exceptionally good 
 return when it is remembered that these crushings are from eight different claims, and 
 from ten or eleven separate reefs. 
 
 RAGLAN, CALLIOPE, NORTON, CANIA, AND KROOMBIT GOLD FIELDS. 
 
 The Raglan Gold Field has been in existence since 1867. At the Old Diggings, 
 the Two-mile Diggings, and the Mount Larcombe Scrub, considerable quantities of 
 alluvial gold have been obtained. The country-rock consists of grey and siliceous 
 slates, and hardened sandstones or quartzites, with occasional conglomerates and 
 limestones. The limestone contains few fossils, but Crinoids are common, and a species 
 of Aviculopecten, like A. multiradiatus, has been detected by Mr. Rands. This species 
 occurs in the Gympie Beds, and the auriferous strata are probabiy of the age of 
 the latter. 
 
 The Duke of Brittany Reef has yielded on an average a little over $-oz. of gold 
 to the ton. About 1,000 oz. were obtained from the reef in a few years. Several other 
 reefs lave been worked from time to time. A copper lode has been opened up near the 
 Old Diggings. 
 
 The Calliope Gold Field was discovered in 1863. “Gold has been obtained in fair 
 quantities in the beds of nearly all the gullies heading from the Boyne Range. Amongst 
 those on the Calliope Falls are the Nuggetty Gully, Dogleg Gully, Ten Men’s Gully, 
 and Gordon’s Gully, all of which run westward into Oakey Creek, in Brennan’s Flat. 
 The gullies at the head of Brennan’s Flat have also yielded gold, and in a gully close to 
 the Sheep Station and running east a great amount of work has been done; the washdirt 
 here was 10 to 12 feet deep. On the slope of the hill patches of alluvial of an older 
 date than that in the gullies are now being worked. 
 
 “Nuggetty Gully, although very patchy, has been the most productive. In 1866, 
 nearly 600 men were at work in this gully alone. The number had decreased to about 
 200 two years later on. Many nuggets up to 5 oz. have been picked up; and an 
 American black is reported to have picked up nuggets weighing 14 oz. and 73 oz. 
 respectively. 
 
108 
 
 “On the eastern or Boyne side of the watershed are Machine Creek, Tucker's 
 Gully, Pancake Gully, and New Zealand Gully. The latter, which was started in 1863, 
 
 has been by far the most productive. A large number of men were employed in it in 
 1872. 
 
 “From over 800 men in the year 1864, the number has gradually fallen so 
 that now (1885) scarcely a score are at present at work on the field. The 
 future of Calliope will depend, therefore, rather on its reefs than on its alluvial 
 deposits. 
 
 “The formation consists of metamorphosed rocks, chiefly of altered grey and 
 greenish slates, with numerous outcrops of limestone and marble.” These have yielded 
 no recognisable fossils. ‘The country-rock is intersected by dykes and patches of 
 serpentine diorite and porphyry.” 
 
 Mr. Rands, in his Report, gives descriptions of the Theresa, King’s Gully, The 
 Company’s, Perseverance, Connemara, John Bull, Alexandra, Mitchell, and Wood’s 
 Reefs, and observes that “up to the present time none of the reefs have had a fair 
 trial. The deepest shaft is not more than 100 feet in depth; and, from the informa- 
 tion I could gather, some of them at any rate have been abandoned for reasons such 
 as want of capital, bad management, high rates for crushing, &c., and not because 
 they did not contain gold in payable quantities, if worked in a judicious and economical 
 manner.” 
 
 The Norton Gold Field is at present the most prosperous of the group, probably 
 for the reason that it has been fortunate enough to attract the attention of men of 
 energy and skill. It was discovered in 1871, but little work was done till 1879, when a 
 machine was erected. 
 
 The formation is a grey, medium-grained granite, which passes in places into 
 syenite and in others into porphyry. 
 
 “The granite is in the form of an eruptive ‘ boss,’ which rises through and sends 
 out veins into the surrounding slate country. 
 
 “The granite is intersected by gold-bearing reefs and voleanie dykes of diorite, 
 porphyry, and dolerite.”’ 
 
 Mr. Rands describes minutely the Advanee, Who’d-have-thought-it, Emu, Never 
 Never, Little Wonder, Chandler’s, Martin’s, All Nations, Galena, and other reefs. In 
 these the gold is associated with iron pyrites, arsenical pyrites, zinc-blende, galena, 
 stibnite (sulphide of antimony), quartz, and calcite. From 1879 to 1884 inclusive, 
 2,766 tons of stone were crushed for 7,883 oz. of gold, but the treatment of the complex 
 mundie proved the chief drawback to the development of the field. Lately, chlorination 
 has been successfully applied to the treatment of the stone, and the field will probably 
 develop steadily in future. 
 
 The country-rock of the Cania Gold Field is deseribed by Mr. Rands as consisting 
 of alternate layers of sandstone, slates, and limestone, the latter of a pisolitie structure 
 and in parts fossiliferous. These rocks are capped by denuded tablelands of ‘“ Desert 
 Sandstone.” The limestones have yielded Corals and Brachiopoda, which render it 
 almost certain that the auriferous strata belong to the same age as the Gympie Beds 
 (Permo-Carboniferous). 
 
 “Colours of gold can be obtained from the drift in the beds of any of the 
 creeks or gullies in the district, and most of them have been worked more or less. 
 On the Cania or Three-moon Creek side of the watershed, the principal workings 
 are the Four-mile Creek and its gullies. This creek has yielded large amounts 
 of gold in rich patches, but it is not at all evenly distributed, and the beds 
 cannot be followed any distance. Lower down on the same or west side of the 
 

 
 109 
 
 ereek is the Moonlight Gully, which has given perlraps the best yields on the field, 
 the gold being evenly distributed along the whole length of it. This and also the 
 Chinaman’s, Starlight, and Daylight Gullies all head from the same hill, around the 
 foot of which the Three-moon Creek bends. Several reefs occur on this hill, some 
 of which are being worked. On the other side of the creek, Paddy’s Gully has proved 
 the best.” 
 
 In the Mount Rose Reef the gold is in white quartz; near the surface 
 it was found in calcite. It is “met with in very rich patches, and at times over 
 100 oz. have been broken down in one patch. All the gold in this reef is coarse 
 in character.’ The Garry Owen and Mount Hope Reefs crushed over 2 oz. to 
 
 .the ton. 
 
 “The Kroombit Diggings, on the other side of the watershed and west of Cania, 
 were discovered in February, 1870, just a month before Cania was opened. Of the 
 gullies on these falls the Roan Colt and Denny’s have, perhaps, proved the best. They 
 head from a small round hill which is itself partially covered with alluvial drift to a 
 depth of 20 feet, which has yielded a fair amount of gold. There is another round- 
 shaped hill about a mile to the east, which has also a similar drift on its suminit. 
 Gullies running also from the hill have been payable to work. The drift on these two 
 hills is evidently of a date anterior to that found in the beds of the present creek or 
 gullies. It is probably of Post-Tertiary age.” 
 
 The above quotations are from Mr. Rands’ “Report on the Gold Fields of 
 Raglan, Calliope, Milton (Norton), and Cania, &c.’’* 
 
 The returns from these fields are very incomplete. Prior to 1877 I have only 
 been able to find records of the output of 1866 and 1868. The best years of the 
 alluvial diggings, as will be seen from Mr. Rands’ report, are omitted. An estimate of 
 2,000 oz. per annum for the eleven omitted years is probably well within the mark, and 
 this, with the recorded output, brings the total yield up to 70,192 oz. 
 
 YIELD oF Raa@uan, Cattiopr, Norton, Canta, AND KroomBit Goip FIErLDs. 
 
 
 
 
 
 
 
 
 
 Year. Stone Crushed. Yield therefrom. Alluvial Gold. Total. 
 Tons. Oz. Oz. Oz. 
 
 1863 to 1865... ind Sef rt ae say, 6,000 
 1866 eae san) vaté ee S66 Sa 8,235 
 1868 ee Age gud iiss ar aaa 3,960 
 1869 to 1876... ees 360 “or wee 16,000 
 1877 ae nur ae 107 1,209 791? 2,000 
 1878 ate ade tics 222 956 329 P 1,285 
 1879 Bes Sia aa 926 1,517 nn T3517 
 1880 wan oa oe 785 3,430 ae 3,430 
 1881 Ape das ese 823 2,072 998 ? 8,070 
 1882 er Bee es a (No returns) es 3,996 
 1883 Ene wae ee 463 1,172 594 1,766 
 1884 wee ats ae 817 1,550 583 2,183 
 1885 “we Bar AD 687 1,469 631 2,100 
 1886 are S00 oe 841 2,166 1,072 3,238 
 1887 50 vse Sc 1,067 2,610 1,170 3,780 
 1888 are ite as 1752 Seu 590 4,321 
 1889 “a xs ae 1,020 2,963 1,184 4,097 
 1890 ane ae ae 8,008 3,409 855 4,264: 
 
 Total *P es 70,192 
 
 
 
 * Brisbane: by Authority ; 1885, 
 
110 
 ROCKHAMPTON GOLD FIELDS. 
 
 (Exctupine Mount Morean.) 
 CROCODILE, ROSEWOOD, MORINISH, RIDGELANDS, AND CAWARRAL. 
 
 The Crocodile Gold Field lies at the foot of the north-west escarpment of the 
 tableland on which Mount Morgan is situated, and can hardly be more than from 1 to 
 300 feet above the sea-level, on the heads of Gavial Creek, which falls into Keppel Bay 
 thus proving, by the way, the falsity of an obstinate superstition among miners to the 
 effect that payable gold cannot be found on the east coast. This belief, or rather its 
 ogical converse, that any gold found on the east coast cannot be payable, has exerted a 
 powerful depressing influence on all such shows, as miners could hardly be induced to 
 give them a trial. The prevailing country-rock is granite or syenite, and in this are the 
 Hector, Who’d-have thought-it, Block and Pillar, Hit or Miss, and other reefs. The 
 St. Gothard and Bonanza are in altered stratified rocks—slates, greywackes, grits, and 
 conglomerates—intersected by diorite dykes. 
 
 At the Rosewood Gold Field the Golden Bar Reef is composed for the most part 
 of calespar and chlorite, in pockets, and coating crystals of calcite. Sometimes there is 
 also a good deal of quartz, and crystalline pyrites occurs in films on the surface of the 
 veins. Some very rich bunches of gold have been obtained in calespar veins in this mine. 
 
 The reef occurs in a diorite dyke, which is mostly altered to chlorite. Rich 
 bunches have also been cbtained in the Caledonian Reef, a large body of quartz with 
 patches and pockets of chlorite, intersecting highly altered sandstone country. 
 
 At Blackfellow’s Gully three reefs—the Homeward Bound, Carnarvon Castle, 
 and Mary Florence—have been worked. 
 
 At Morinish the Welcome Reef has been worked to a depth of over 350 feet ina 
 country-rock of fine-grained serpentinous greywacke. The reef is of quartz, with iron 
 pyrites, arsenical pyrites, a little galena, and a very little zine-blende. It has been 
 worked for many years with fair success. 
 
 At New Zealand Gully is the North Star Mine, in porphyry country. 
 
 At Cawarral the Galawa, Annie, Helena, and Annie Halliday, in serpentine 
 country, have yielded good returns. The Cawarral serpentine, as has already been 
 shown, is merely a product of ‘the metamorphism of sedimentary rocks belonging to the 
 Gympie J’ormation. 
 
 Most of these small fields have yielded a good deal of alluvial gold. A nugget 
 weighing 258 oz. 11 dwt. was found at Mount Wheeler (Cawarral). 
 
 The output of the various Rockhampton Gold Fields cannot be correctly given, 
 as the earlier records are lost in the mists of an antiquity of over thirty years. In 
 1866, the Warden estimated the amount of gold at 1,000 oz. per week—52,000 oz. for 
 the year. In 1867, the amount is given at 83,739 oz. In 1868, the total is given at 
 25,505 oz., of which 8,982 oz. were the yield of 7,564 tons of stone crushed. A total 
 of 111,244 oz. is thus accounted for in three of the years previous to 1877, when returns 
 began to be regularly published. It is probably well within the mark to assume that the 
 total yield for the period amounted to about 200,000 oz. From 1885, or, perhaps, from 
 1884 to 1887, the returns from the field are mixed up with those from Mount Morgan. 
 In 1887 the yield for the whole of the fields, excluding Mount Morgan, was estimated 
 by the Warden at 1,600 oz. In 1888, the total, including Mount Morgan, is estimated, 
 at 117,800 oz, but the amounts from the different fields are not stated. In 1889 the 
 yield from mines in the district, other than Mount Morgan, is estimated at 2,130 oz., 
 but this is stated to be “exclusive of alluvial.” In 1890, the yield from mines other 
 than Mount Morgan is estimated at 6,181 oz. 
 

 
 
 
 sal 
 
 YreLp oF Rocknampron Gorp Frenps (Exclusive of Mount Morgan). 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 Year. Stone Crushed. Yield therefrom. Alluvial Gold, Total. 
 Tons. Oz. Oz. Oz. 
 1866 he ee ae 5s uae ia 52,000 
 1867 Gress wae 500 Ae nate ssid 33,739 
 1868 see ioe Is 7,564 8,982 ae 25,505 
 111,244 
 Estimated amount prior to 1877 cee a mis ea a sie wa 88,756 
 Total he Sad a ine 200,000 
 1877 ay ave Abe eae es one 2,350 
 1878 Res mae ph 1,120 733 wate 2,071 
 1879 fo Pr oe ae nee oe 707 
 1880 ae aes Awe ‘sie oe oe 1,353 
 1881 nee vale ar ne an ane 2,132 
 1882 ee ay wee 1,092 2,016 Le 2,107 
 1883 we mee cies Sar nae 5,591 
 1884 ARG are Ae sag ra ade * 
 1885 a os ere ay tae ae Ti 
 1886 ies we eae sor 49,086 ee 40 
 1887 ce be Ane 17,645 85,205 100 1,600 
 1888 Abe ae Ses aie a ee say, 1,600 
 1889 His ae oat nae ay (Not estimated) 2,130 
 1890 ae acti AY ae af (Not estimated) 6,131 
 opal mane ni 227,773 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 * “ Work at a standstill, except as regards Mount Morgan.’’ Warden, in Annual Report, Department of Mines. 
 + No estimate, although several mines crushed. 
 + No estimate, although ‘‘ great activity prevailed.” 
 
 YATTON GOLD FIELD. 
 
 The recentiy opened goldfield of Yatton is in a dioritic country-rock, intersected 
 by dykes of silicated felsite. Some of the auriferous reefs, such as the St. Catherine, 
 follow the usual laws of such deposits, but the majority are peculiar as regards the 
 conditions under which the gold is found. The gangue-stuff, which is generally com- 
 posed of brecciated lumps of diorite is veined with calcite and decomposed concretionary 
 carbonate of lime, and occasional aggregations of carbonate of iron (siderite) and 
 decomposed orthoclase felspar are met with. Some of the stone, composed of mixed 
 quartz and reddish ferruginous carbonate of lime, shows gold very freely. The gold is 
 flaky, like goldleaf. The reefs are as yet too undeveloped to say much about. 186 
 tons crushed in 1877 gave 74 oz. of gold, but these figures give no idea of the yield of 
 the field, as the richest parts of many of the reefs probably never passed through the 
 stampers. A good deal of alluvial gold had been taken from Yatton seven years before 
 the proclamation of the field. The reefs are not yet sufficiently developed to give a true 
 idea of their value, as they are mostly of a character of which miners have had little 
 experience. 
 
 GOOROOMJAM DIGGINGS. 
 
 Gooroomjam is situated on that portion of the Bunya Range which divides the 
 
 -sources of the Brisbane River from those of the Burnett. The diggings are confined 
 
 to two gullies that descend from either side of the range. Monarrumbi Creek is worked 
 for about half-a-mile in length, and the Dry Gully for even a less distance than this. 
 The area mined upon consists entirely of greenstone, with the exception of the lower 
 
112 
 
 portion of the workings on Monarrumbi Creek, where massive hornblendic slates crop 
 out at the foot of the range on the north side of the creek, and granite on the point of 
 the spur constituting the south bank. But I believe that the little quantity of gold 
 found here has travelled from the tract of greenstone above, and that the whole of the 
 gold has been derived from this latter rock. The only instances of vein quartz, locally 
 termed “reefs,” were in the Wild Horse and White’s Claims, both being in greenstone.* 
 
 WARWICK GOLD FIELDS. 
 LUCKY VALLEY, TALGAI, CANAL CREEK, AND PIKEDALE. 
 
 These small goldfields have never attained to any importance. Mr. C. D’Oyly H. 
 Aplin, in his “‘ Report on the Auriferous Country of the Upper Condamine,’+ says :— 
 “Talgai, Thane’s Creek, and Canal Creek are comprised within one continuous area of 
 similar formation (probably Lower Silurian),{ but between this and its eastern develop- 
 ment at Lucky Valley there intervenes, along the immediate valley of the Condamine, 
 a strip of about twenty-five miles of country occupied by sandstones, gravels, and con- 
 glomerates, belonging to the Coal Measure Series”’ [Ipswich Formation]. 
 
 Lucky Valley is entirely an alluvial diggings. 
 
 Copper lodes, as well as auriferous mundic reefs, occur at Pikedale. 
 
 In a quartz vein on Duffer Gully (Lucky Vailey) there are found “small, bright, 
 foliated metallic plates and scales of tellurium, in which gold may be seen imbedded.” § 
 
 YIELD OF WaARWwIcK GoLpD FIELDs. 
 
 
 
 
 
 
 
 
 
 
 
 Year. Stone Crushed. Yield therefrom. Alluvial Gold. Total. 
 Tons. Oz. Oz. Oz. 
 1867 a5 790 988 ve 988 
 1868 to 1876 ah (No returns) (No returns) wae 
 1877 fa 325 390 (No returns) 390 
 1878 572 736 (No returns) 736 
 1879 40 60 er 60 
 1880 199 160 (No returns) 160 
 1881 416 826 (No returns) 326 
 1882 * 5. 648 648 (No returns) 648 
 1883 to 1886 sie (No returns) (No returns) ane 
 1887 Kes 48 72 485 557 
 1888 =r aes (No returns) (No returns) es 
 1889 sn (No returns) a 521 
 1890 1,854 149 2,003 
 Total 4,389 
 J. 
 
 
 
 *C. D’O. H. Aplin, Report of the Government Geologist, Southern Division. Brisbane: by 
 Authority : 1869. 
 + Brisbane: by Authority: 1869. 
 ~ Mr. Aplin does not give a list of the fossils on which this determination is based, and says that 
 ‘in general aspect they resemble the fossils of Gympie.” 
 Aplin. 
 

 
 CHAPTER IX. 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 THE GYMPIE FORMATION OUTSIDE OF THE TYPE DISTRICT—continued. 
 
 InotupiIna Hop@xinson, Parmer, Motnr ALBion, SILVERFIELD, WATSONVILLE, AND CHILLAGOE. 
 
 Mineral Areas—viz., Hodgkinson Gold Field, Northcote Antimony Mines, Mulgrave Gold Field, 
 Palmer Gold Field, Cannibal Creek Tin Field, Mitchell Antimony Mines, Mount Albion 
 and Chillagoe Silver Fields, Dry River Silver Field, Nebo Gold Field, and Sellheim Silver 
 Field. 
 
 The geological position of the Hodgkinson Gold Field has long been a debatable 
 point in my mind, but I can now see my way to include it, at least provisionally, in the 
 Gympie Beds. 
 
 This goldfield was described in detail by the Writer ina Report * accompanied 
 by two maps. 
 
 The stratified rocks of the Hodgkinson vary in fineness from shales to 
 conglomerates. The shales consist of pure blue clay, sometimes (as for instance at the 
 Rob Roy Mine) blackened by carbonaceous matter. The clay is divided into thin 
 lamine by the planes which mark the pauses in the process of deposition. Slaty 
 cleavage is not entirely unknown, but it is so rarely met with and so uncertain in its 
 direction, that it may be presumed that pressure of the sort which results in the 
 production of cleavage has been very feebly exerted in this region. Alternating with 
 the shales are strata of greywacke, whose materials are essentially the same although 
 less comminuted. The component grains or granules of the greywackes have been partly 
 derived from a basic felspar and partly from a hornblendie rock. The felspatho-horn- 
 blendic matrix contains minute flakes of mica and grains of quartz, both apparently 
 derived from a granitic rock. According to the frequency and size of the quartz grains, 
 the greywackes pass by fine gradations into grits and conglomerates. The latter, 
 however, contain, besides quartz pebbles, pebbles of quartzite or hardened siliceous 
 sandstone, porphyry, lydian-stone, dark shale, and limestone. 
 
 By carefully noting the dip and strike of the strata, wherever they appear at the 
 surface in gullies or on hilltops, and laying down their direction and degree on the 
 maps, a tolerably clear idea of the structure of the goldfield has been obtained. The 
 different strata do not present such marked characteristics that they can be traced with 
 confidence for long distances, although some of the conglomerates in Glen Mowbray 
 have been followed for more than a mile. Conglomerates, however, are from their very 
 nature—being the product of strong currents and powerful attrition—apt to be of very 
 local occurrence. 
 
 Within the area embraced by the large map (the neighbourhood of Thornborough 
 and Kingsborough), there is a marked connection between the geological structure and 
 physical features of the field. This probably holds equally true of the outside districts, 
 which have not yet, however, been mapped. 
 
 
 
 * Brisbane : by Authority ; 1884, 
 
114 
 
 The strata strike, on the whole, from north-west to south-east, the denuded edges 
 coming to the surface in that direction. Their dip is usually towards the north-east, 
 and ata high angle, approaching the vertical. But the lines denoting the outcrops of the 
 strata, as will be seen from the map, bend or “bag” southward along an axial line passing 
 to the west of the township of Thornborough. It is impossible to estimate exactly the 
 thickness of the series of strata to which the goldfield belongs, as neither top nor bottom 
 has yet been detected, and, moreover, the apparent thickness may be exaggerated by 
 unsuspected replications among the denuded beds; but a minimum thickness at least 
 may be arrived at with some confidence by assuming that, allowing for replications, and 
 even for possible faults, the average dip to N.E. is no more than 65°. On this assump- 
 tion a thickness of 4,000 feet may be presumed for the strata cropping out between the 
 horizon of the Amy Moore Mine and the north-east edge of the large scale map, as 
 measured to the south-east of Kingsborough. Measuring downward from this same 
 horizon at Peak “N,” in the Mount McGann Range, south-westward to Mount Grant 
 (a line where the apparent thickness is not affected by the bending or bagging above 
 referred to), a further thickness of at least 17,000 feet of strata is met with. 
 
 The detailed “Study in Stratigraphy ”’ which the preparation of the large map 
 implies has revealed nothing to suggest the idea of any break in the continuity of the 
 deposition of the whole series of at least 21,000 feet of strata, unless it be the gathering, 
 at the head of Columbia Creek, of a portion of the series which at the mouth of 
 Caledonia Creek, only five miles distant, measures (at 65° of estimated average dip) 
 about 10,000 feet, into a space which can contain, although the strata are vertical, no 
 more than 1,300 feet. But I am inclined to think that the phenomenon may be 
 explained by a thinning out of the sediments towards the south-east, though possibly 
 the effect may be aided by a fault having a downthrow to the north-east. 
 
 The nearly parellel valleys of Caledonia Creek (Glen Mowbray) and the Hodg- 
 kinson River are bounded on the right or north-eastern side by the Mount McGann 
 Range, and on the opposite side by the Mount Robert Range. These ranges have had 
 their trend determined indirectly by the forces which compressed the strata of the 
 district from south-west to north-east, and threw them into long folds from south-east 
 to north-west. After the strata had been compressed into nearly as small a compass 
 as they would go into—z.e., till they became ncarly vertical—the further operation of 
 the same pressure resulted in the formation of fissures along lines of weakness, 
 which lines of weakness were found in the bedding-planes dividing the upturned 
 strata from one another. These fissures, which are nearly, but not exactly, parallel 
 with the outcrops of the strata, have been filled with a rock of great hardness, 
 which, by its power of resisting denudation, has given rise to the Mount McGann 
 and Mount Robert Ranges. Both of these ranges occur in zones in which the 
 hard rocks in question are closely grouped together, while the intervening softer 
 “eountry” has been channelled by the Hodgkinson River and Caledonia Creek 
 into deep valleys. The material with which the fissures are filled forms veins or 
 dykes, from three to forty feet in width, of pure silica in almost all of its various forms. 
 It frequently resembles quartzite, and occasionally passes into ribbon-jasper or chalce- 
 dony. The veins are often so laminated parallel to their sides as to suggest that they 
 may be beds rather than veins, but the mode in which they now and then cut across the 
 adjacent strata,although preserving a general parallelism, sufficiently disproves this theory. 
 Crystallisation is comparatively rare, and the lamination seems to imply deposition of 
 silica during the passage of copious sheets of hot water charged with the mineral in 
 solution rather than the segregation of the silica from the surrounding strata. The veins 
 (which they hardly are in the usual sense of the word), as laid down on the map, are very 
 
 
 

 
 115 
 
 striking; but in nature they are more remarkable still. They can be followed from hilltop 
 to hilltop, forming at times rough insurmountable walls a hundred feet in height 
 —as, for example, in the peaks west of Mount Tenison Woods. Jn other places denuda- 
 tion has left their remains on hillsides or hilltops in the form of huge cubes of hard 
 quartzite, from which the surrounding softer rocks have crumbled away. These cubes 
 stand up weird and solitary, like the “perched blocks” of Alpine and Arctic lands. The 
 linear persistence of the veins in question is very remarkable. One, for instance, has 
 been traced (with a few breaks) from Mount McGann to the head of Tyrconnell Creek, 
 a distance of over six miles. The two veins intersecting Mount Robert have been 
 followed for four miles each. In these and many other cases the tracing of the veins 
 was abandoned for no other reason than that the limit of the map had been reached. 
 Similar veins, it may be here observed, have been noted by the Writer in the Cloncurry 
 and Leichhardt region, where they attain still more gigantic proportions. The veins of 
 the Cloncurry and Hodgkinson resemble the dolerite dykes of Scotland and Ireland 
 more than the ore-charged reefs of Australia. The Hodgkinson veins, I have been 
 informed, contain rare and minute quantities of gold. I have not been able to verify 
 this information, and suspect that the gold may have come from reefs adjacent to the 
 veins. Specular iron ore, brown hematite, and binoxide of manganese are not uncom- — 
 monly found in the cavities of the larger veins. 
 
 In a conglomerate on the hillside, opposite the Glen Mowbray Machine, there 
 occur some large oval pebbles or shingles of black shale. The shingles strongly resemble 
 the Graptolite Shales of Victoria and the Uplands of the South of Scotland. But they 
 are also quite undistinguishable from the beds of dark shale which lie beside, and 
 geologically both above and below, the conglomerate bed. I split open a great number 
 of the shale shingles in search of graptolites, but without success. They yielded instead a 
 number of reed-like plant-impressions, invariably too indistinct for determination. 
 
 Near the northern boundary of the township of Thornborough is the Chance 
 Tunnel. The locality is about a mile south of the conglomerate in Glen Mowbray, and 
 the strata cut in the tunnel occupy a horizon which may be estimated at 4,620 feet 
 below that of the conglomerate. They consist for the most part of dark-blue shales 
 (commonly but improperly known as slates), with alternations of hard, gritty grey- 
 wackes and a few bands of fine conglomerate. The fine-grained greywackes yielded a 
 “ petrified snake,” which was sent to the Queensland Museum, and pronounced by Mr. 
 C. W. de Vis to be a Lepidodendron, probably LZ. australe, McCoy.* I visited the spot 
 afterwards, and saw some flattened stems and twigs, which may have belonged to 
 Lepidodendron, but from which all the characteristic markings had disappeared. My 
 visit left no doubt on my mind regarding the dona fides of the discovery. I found 
 among the shales numerous casts of crustacean or molluscan tracks, some reed-like 
 plant-impressions, and a fragment of carbonised wood. 
 
 Even if the shale pebbles or boulders or shingle (as the case may be) of the 
 Glen Mowbray or other similar conglomerate should in future yield recognisable fossils, 
 T should not necessarily regard the fossils as “derived”? from some older formation 
 which had been upheaved and subjected to denudation during the period marked by the 
 deposition of the conglomerate. On the contrary, I should believe the fossils to be of 
 _ practically contemporaneous origin. I believe the plant-remains of the Glen Mowbray 
 shingles must have been derived from a bed of shale which formed a part of the same 
 formation. In my field experience nothing is more certain than that fragments of a 
 given shale bed will be found in any succeeding bed of conglomerate. The explanation 
 
 
 
 * This has since been confirmed by my Colleague, who was allowed, by the courtesy of Mr, De Vis, 
 to examine the specimens in the Queensland Museum, 
 
116 
 
 is, I believe, to be found in the sun-drying and peeling-off of flakes of the shale and 
 their subsequent partial rounding by attrition. I say this by way of caution against 
 hasty conclusions from future discoveries. In the very probable event, for instance, 
 of the discovery in shale-shingles of a determinable fossil—say, Lepidodendron australe 
 —the conclusion would be that the conglomerate containing the shingle was deposited 
 in a geological age subsequent to the deposition of the shale containing Lepidodendron 
 australe, and, in my belief, the conclusion would be erroneous. 
 
 At the intersection of the road from Thornborough to Glen Mowbray with that 
 which leads up to the Pioneer and Tichborne Mines is the outcrop of a bed of con- 
 glomerate, in which pebbles, up to six or eight inches in diameter, are closely packed 
 in a matrix of greywacke. Of these pebbles some are of greywacke, the majority 
 quartz, and a fair proportion blue coralline limestone. Similar limestone pebbles are 
 found in conglomerates in a number of other places—e.g., on the hill west of the City 
 of Dublin Reef, on the roadside in Glen Mowbray, near the junction of the Thorn- 
 borough and Kingsborough roads, in the gully west of the shambles in Glen Mowbray, 
 and in Tyrconnell Creek, north of the Honest Lawyer. 
 
 As in the case of the shale-shingles of the Glen Mowbray Conglomerate, I con- 
 sidered it very doubtful whether the fossils in the limestone pebbles were really 
 “derived” from an older formation, having observed that the shingles on the Pacific 
 coast of the present day contain numerous pebbles and boulders of coral drifted from 
 the Barrier or other reefs. In this view I was subsequently confirmed by the discovery, 
 about a mile and a-half south-west of Beaconsfield, of a conglomerate with similar 
 pebbles containing similar fossils, almost immediately adjoining a bed of limestone which 
 has been quarried for mortar for the Antimony Smelting Works at Northcote. This 
 bed of limestone is vertical, four feet at least in thickness, and strikes north-north-west, 
 as do all the strata in the neighbourhood. The limestone was found to contain a number 
 of corals and shells, among which my Colleague has recognised Pachypora, sp. ind., and 
 Cyathophyllum, sp. ind. (Pl. 8, f.10). Without attempting to name any more of the 
 corals, which are in indifferent preservation, it is easily seen that several species are 
 common to the limestone bed and to the limestone pebbles in the conglomerate. The 
 corals which weather out in relief from the limestone pebbles of the conglomerate may 
 therefore be ranked as contemporaneous with the strata of the goldfield. 
 
 The discovery of Lepidodendron in the Gympie Beds at the Training Wall 
 Quarries, Rockhampton, removes one formidable objection to classing the Hodgkinson 
 Beds with the Gympie Beds. As long as Lepidodendron was believed to be confined to 
 the Star Beds, its occurrence in the Hodgkinson strata seemed favourable to placing the 
 latter on a horizon near the former. We have here a second instance of the occurrence 
 of Lepidodendron associated with a marine fauna in one and the same bed.* 
 
 The auriferous reefs of the Hodgkinson are well defined, and are divisible into 
 two groups or orders. Those of the first group coincide in their strike with the strike 
 of the strata in which they occur. To this group belong the Tasmanian, North Star, 
 Outward Bound, Amy Moore, Vulcan, Britannia, Caledonia, Forget-me-Not, Von 
 Moltke, Lady Mary, Mark Twain, Rob Roy, Garry Owen, Tyrconnell, Black Prince, 
 Henry Grattan, Commodore, Lizzie Redmond, Hero, Pioneer, Hope, and others. In all 
 the members of this group a general law may be observed. They underlie at right angles 
 to the dip of the strata. This circumstance can only mean that the fissures were produced 
 by the same pressure that upturned the strata. Each stratum would break along a 
 plane of least resistance, which would be found at right angles to the planes of bedding. 
 
 * See Annual Report of the Department of Mines, N.S.W., for 1889, p, 239, 
 

 
 117 
 
 The second group, which comprises the Bismarck, King Atilla, Lady Anne, 
 Providence, Flying Pig, Tichborne, Idaho, Explorer, Great Northern, Devon and Corn- 
 wall, Empress of India, Alliance, Mowbray, Honest Lawyer, Fourth of July, Columbia, 
 and Eureka, runs mainly north and south and at right angles to the lines which denote 
 the outcrops of the stratified rocks. Their underlie is always to the east. It is 
 probable that they belong to a period subsequent to the first series of fissures. 
 
 The gold occurs in a matrix of laminated quartz, without much pyrites or galena 
 (except in the case of some of the mines of the Hastern Hodgkinson). There is 
 consequently little difference in the productiveness of the stone above and below the 
 water level. Blanks are met with here and there in most of the reefs—i.e., spaces con- 
 taining neither gold nor quartz, but only a breeciated gangue of sandstone and shale 
 fragments. The gold almost always occurs in rather narrow “shoots,” most of which 
 die out (although the quartz may continue) at less than four hundred feet in depth. 
 There is, however, no reason to doubt that at greater depths other shoots will yet be 
 discovered. 
 
 In addition to the reefs around the townships of Thornborough and Kings- 
 borough, Deep Creek, Woodville, the Eastern Hodgkinson, and Northcote are or have 
 been important centres of mining industry. Antimony lodes occur at Woodville and 
 Northcote. At the latter large smelting works have been erected. 
 
 The strata of the Palmer Gold Field are in all probability of the same age as those 
 of the Hodgkinson Gold Field. Between the Idaand Maytown the shales or slates and 
 sandstones have a pretty uniform north-north-west and south-south-east strike, and are 
 nearly vertical, with a slight dip to west-south-west. From Maytown, down the Palmer 
 for about a mile, similar rocks, also nearly on edge, strike mainly north and south, with 
 a slight dip to the west. Farther west the character of the stratified rocks changes ; 
 they become of a more altered type, consisting mainly of slates and schists. A limestone 
 bed of immense thickness belonging to the same series runs south-south-east from 
 Palmerville for at least twenty miles towards the Mitchell. I failed to obtain any 
 fossils from this limestone, which is generally blue and unaltered, but at times becomes 
 a grey crystalline marble. The same limestone is traceable from Palmerville northward. 
 On the east side of the Cooktown and Palmerville Road, about four miles north of 
 Palmerville, the limestone is vertical, and strikes north and south, and is accompanied 
 by vertical slates (with a similar dip and strike), which occupy the floor of the valley 
 or pass through which the road and telegraph line are carried. The limestone here is a 
 grey, crystalline marble, although its surface is blackened by a crust of lichens. The 
 only fossils observed were Crinoid stems, too imperfectly preserved for specific or even 
 for generic determination.. The limestone forms a cliff of about a hundred feet in 
 height, which is weathered into the most fantastic and even grotesque shapes. The 
 strata of this formation are succeeded unconformably by the Desert Sandstone on the 
 right bank of the Palmer, from Palmerville up to Maytown. 
 
 Between Maytown and the head of Limestone Creek, a tributary of the Mitchell, 
 the slates and greywackes of the goldfield strike for the most part north-west and south- 
 east. ‘I'he whole of the so-called “‘ Limestone”? District shows little but slates or shales 
 and sandstones or greywackes, with a nearly vertical dip and a north-and-south strike. 
 Occasionally beds of flinty lydian-stone are interstratified with the shales and greywackes. 
 Between the mouth of Limestone Creck and the St. George and Mitchell Rivers, is a 
 conglomerate containing pebbles of blue limestone. This conglomerate is exactly similar 
 to the conglomerate of Glen Mowbray already described, and the shales and greywackes 
 themselves bear such a strong lithological resemblance to those of the Hodgkinson 
 Gold Field that the conclusion is irresistible that they are part of the same deposit. 
 
118 
 
 The country-rock of the lead, silver, and tin-bearing region of Mount Albion, 
 Irvinebank, Dry River, and part of Watsonville probably belongs to the same age as 
 the Hodgkinson and Palmer Gold Fields. At Mount Albion the strata consist of thick- 
 bedded, fine, grey, hard, siliceous sandstones, sometimes approaching quartzite, and always 
 somewhat pyritous, and grey and dark shales. These rocks, in the mountain on which 
 the Mount Albion, Lady Jane, and Barossa Silver Mines are situated, are intersected 
 by numerous faults, which traverse the field in every direction, and cut it up into small 
 pieces, the dip and strike being totally different in each of these sections. 
 
 The sandstone of No. 1 Lady Jane Shaft and the shale of the Mount Albion Mine 
 at the depth of 114 feet are plentifully marked with plant-impressions, which, however, 
 are quite undistinguishable. 
 
 At Silverfield, about a mile and a-half south-south-east of Mount Albion, similar 
 strata, with, however, a larger proportion of shales, form the matrix of argentiferous 
 galena lodes. The strata strike west-north-west and underlie at high angles to south- 
 south-west, but do not appear to be disturbed by faults to anything like the same extent 
 as the Mount Albion strata. 
 
 Similar strata extend from Mount Albion through Irvinebank to the Dry River 
 at Newelltown, a distance of about forty miles. At Irvinebank numerous tin lodes occur 
 in these rocks. At the Dry River numerous argentiferous galena lodes, some copper 
 lodes, and a lode of magnetic ironstone occur among grey and black slates or shales and 
 greywackes, together with a bed of blue limestone, striking north and south. I could 
 not find any fossils in the strata worth preserving, although the limestone showed traces 
 of corals on weathered surfaces. - 
 
 In the Great Western District, near Watsonville, a group of tin-mines lies in a 
 band of slates and greywackes, intervening between the granite of Watsonville and the 
 porphyry of the dividing range between the Walsh and Herbert Rivers, in the latter of 
 which the majority of the tin-mines of the Western District are situated. The band of 
 greywackes and slates extends from east to west, broadening considerably to the east. 
 The strata dip for the most part at comparatively low angles to the south-west. The 
 deposits of tin and copper ores in this district have a marked tendency to leave the 
 fissure lodes and replace to some extent the material of the stratified rocks. 
 
 In the neighbourhood of Mount Albion a series of shales, sandstones, and grits 
 replace the porphyry, which has extended for some distance to the east. In this 
 formation are the silver-lead mines of Mount Albion and Silverfield. These strata have 
 a general east-north-east and west-south-west strike, while their dip may be either to 
 north-north-west, or south-south-east, or vertical. In Mount A!bion itself (the moun- 
 tain), the sandstones and grits predominate, and the strata are intersected by a network 
 of faults, between which they strike and dip in every direction. At the surface, the 
 siliceous sandstones and grits of Mount Albion have an almost vitrified appearance, 
 and might almost be classed as quartzites, and often weather in large spheroids, like 
 granite blocks. When followed down in the mines, however, they have much more the 
 appearance of ordinary unaltered rocks, the difference being apparently, to some extent 
 at least, due to the loss of the “ quarry water ”’ in the strata exposed at the surface. 
 
 The road from Mount Albion to Georgetown, which runs at first southward down 
 Albion Creek and then westward down Oakey Creek to near the junction of the latter 
 with Gibbs Creek, traverses sandstones, grits, and shales like those of Mount Albion, 
 dipping on the whole to the 8.E. at about 50°, although the strata are much disturbed 
 by faults, and the dip is frequently reversed. Near the last crossing of Oakey Creek 
 the stratified rocks are replaced by a mass of porphyry, with round clear blebs of 
 quartz, not very large orthoclase crystals, and.a dark mineral, which may be weathered 
 

 
 119 
 
 hornblende, in the interstices. This rock weathers deeply, but quite differently from 
 either the Herberton porphyry or the Watsonville granite. The surface is bestrewn 
 with angular blocks, generally of not more than two cubic feet, with rounded angles. 
 The porphyry continues to about one mile beyond the junction of the Georgetown coach 
 road and the Chillagoe road, where the sandy grits and conglomerates of the Mount 
 Albion type are again met with. The stratified rocks occupy the whole of the Chillagoe 
 road from this point down Emu Creek, and across Sandy and Oakey Creeks, a distance 
 of about thirteen miles. At the first crossing of Emu Creek the grits occur in very 
 thick beds, and, as well as the accompanying shalcs, are nearly vertical, with a slight dip 
 to the south. At the crossing of the creek half-a-mile beyond Leakey’s Creek the 
 Mount Albion grits are a good deal hardened. Blocks of a coarse conglomerate (with 
 a gritty matrix and large pebbles of quartzite) have been carried down the creek. 
 Where the road next crosses the river I ascended a mountain on the left bank, and 
 found it to be composed of grits altered to quartzites, with some limited (? intrusive) 
 masses of porphyry. 
 
 At the 32-mile telegraph post, which is near the road, porphyry rocks are again 
 met with, at the foot of what is known as the Feather-bed Range. Ascending the 
 range by the road, the mass of the range is found to consist of hornblendic granite, 
 which is replaced by shales, sandstones, grits, and conglomerates on the head of 
 Koorboora Creek, a tributary of the Tate. 
 
 From Koorboora Creek westward by the Koorboora Camp are massive altered 
 grits and conglomerates, with a matrix resembling quartzite and containing some grains 
 of quartz and some of plagioclase felspar. Near the head of the creek on which the 
 Koorboora Camp stands, these rocks are intersected by dykes of acidic felstone. The 
 stratified rocks continue along the road west-north-west to between Bismarck and 
 Granite Creeks. Occasionally the grits are somewhat ferruginous. At other times 
 they occur in thick beds, and are sometimes pebbly or conglomeratic, with a quasi- 
 vitrified matrix, and weather in rude spheroids like granite. 
 
 Between Bismarck and Granite Creeks the road crosses a belt of coarse porphyry 
 of the Herberton type, intersected by dykes of compact yellow felstone. The porphyry 
 here appears to pass into true granite, containing sparse crystals of black mica 
 (biotite). From this point to Mount Lucy granite is the prevailing rock seen in the 
 neighbourhood of the road. 
 
 A little beyond Mount Lucy the road to Muldiva strikes off to the left (south- 
 west). At the junction of the roads beds of limestone are for the first time met with. 
 Along the Muldiva road limestones are seen at intervals interbedded with thin flaggy 
 quartzites, which latter are sometimes honeycombed with cavities from which limestone 
 has weathered. These strike N. 20° W. and dip at high-angles to W. 20° S. In about 
 four miles from the turn-off of the road, and near the Muldiva Camp, the granite 
 recommences. The road from Muldiva to Chillagoe, which joins the main road about 
 a quarter of a mile east of Gorge Creek, also traverses strata of limestone and 
 quartzite. 
 
 From Gorge Creek by the road north-westward to Zillmanton, and for a few 
 miles beyond, the country presents alternations of comparatively flat land with ranges 
 of limestone, which stand from one to four hundred feet above the level of the flats. 
 The limestone is apparently in vertical beds, which strike on the whole to north-west 
 and south-east, although there are evidently many changes in the strike. In some cases 
 I am pretty certain that the trend of the short “ ranges” does not correspond with the 
 strike of the upturned beds. These strata between the limestones are comparatively 
 rarely exposed, being covered, as a rule, by a considerable depth of red soil. 
 
120 
 
 In the neighbourhood of Redcap the limestone beds, as shown by quartzites 
 interstratified with them, strike west-north-west and dip at high angles to north-north- 
 east. In this district many thick beds of coarse conglomerate are interbedded with 
 the limestones and quartzites. 
 
 Between Zillmanton and Dargalong Camp, which lies about six miles to the south, 
 a thick bed of limestone is first crossed on the left bank of Stockman’s Creek. For the 
 next two miles the track crosses grits, highly altered coarse conglomerates, and fine 
 shales, the grits being recognisable without hesitation as of the Mount Albion type. To 
 these succeed mica-schists, with a few interstratified beds of altered Mount Albion 
 grits. In about a mile the mica-schists pass into gneiss, and ultimately into micaceous 
 granite. For two miles further the track crosses granite country with numerous quartz 
 reefs. At the end of the two miles mica-schist recommences, and in it, near the junction 
 of the granite, are the silver lodes of the Delaney or Dargalong group. 
 
 There is no question in my mind of the continuity of the whole series of stratified 
 rocks met with between Mount Albion and Zillmanton. The grits met with throughout 
 the whole series are so characteristic and so peculiar that these rocks must have been 
 laid down during the continuance of almost identical physical conditions, or, in other 
 words, during a single geological period. The purely mechanical character of the 
 deposits to the east of Mount Lucy is, however, in strong contrast to the conditions 
 which must have prevailed during the deposition of the limestones north-west of Mount 
 Lucy. But the interbedding of the Mount Albion grits with the Chillagoe lime- 
 stones shows that the regions east and west of Mount Lucy, although forming different 
 horizons, belong to the same geological period. In the absence, or almost entire absence, 
 of detailed mapping, it is difficult at present to be certain of the relative ages of the two 
 horizons, but from what dips have been observed I lean to the opinion that the calcareous 
 horizon is higher than the purely mechanical. 
 
 The limestones are generally semi-crystalline or crystalline in texture, passing into 
 white marbles, and yield few and very imperfect organic remains. Near the Dorothy 
 Mine I obtained some specimens of Corals and Encrinite stems, but from their state of 
 preservation I do not think that the most expert Paleontologist could determine either 
 genus or species. Similar fossils were obtained from the quartzites associated with the 
 limestones near Zillmanton, but in no more recognisable condition. A section of this 
 fossiliferous rock shows, under the microscope, that some erystalline éalespar is still 
 entangled in the silica skeleton, but reveals no trace of organisms. I am strongly 
 inclined to believe that the Chillagoe Limestones will prove to be continuous with the 
 immense beds of limestone extending from the Mitchell, near its junction with Lime- 
 stone Creek, through Palmerville, across the Palmer, and along the Palmerville and 
 Cooktown Road. I have elsewhere* given my reasons for believing in the identity of the 
 strata of the Palmer and Hodgkinson Gold Fields, and I think there is every probability 
 that the Chillagoe and Mount Albion Beds will prove to belong to the same series. It 
 may be observed that the Mitchell and Palmer Limestone bears a very marked lithological 
 resemblance to the limestones of Chillagoe, and that the only fossils as yet recorded 
 from the former belong to the same two classes as those obtained from the latter— 
 viz., Corals and Encrinites—and are in the same unsatisfactory condition. The lime- 
 stones of both regions, as well as the associated strata, present, as regards organic 
 remains, a most striking contrast to the Devonian Limestones of the Broken River 
 and the Burdekin, both of which teem with Corals and Brachiopods in perfect pre- 
 servation. 
 
 * Preliminary Report by R.L.J. on Limestone District, part of the Palmer Gold Field. Brisbane : 
 by Authority : 1888, p. 1. 
 
——— 
 
 a 
 
 
 
 121 
 
 In the Hodgkinson Gold Field, among the shales which alternate with sandstones, 
 grits, and conglomerates, Lepidodendron australe, McCoy, has been detected. This plant 
 is characteristic of the Star Beds (Carboniferous) and of the lower portion of the 
 Newcastle (N.S.W.) Coal-Measures. The shales, grits, and conglomerates of the 
 Hodgkinson probably represent the series of similar rocks—which, however, are 
 somewhat more altered—extending from Mount Albion to Mount Lucy, although 
 in the latter the few plant-remains which have been discovered are not in recognisable 
 condition.* 
 
 On the whole, the stratified rocks of the Mount Albion and Chillagoe Districts 
 must for the present be regarded as equivalent to the Palmer and Hodgkinson Beds, and 
 referred to the Gympie Division of the Permo-Carboniferous system. They pass, as has 
 already been seen, into mica-schists, and finally into granites.* 
 
 A SECOND GROUP OF MINES IN CONNECTION WITH THE GYMPIE 
 FORMATION OUTSIDE OF THE TYPE DISTRICT. 
 HODGKINSON GOLD FIELD. 
 
 This goldfield extends from the divide between the head of the Hodgkinson 
 River and Leadingham Creek (an affluent of the Walsh River), north-westward for 
 about forty miles down the valley of the Hodgkinson. It has already been sufficiently 
 described in a previous portion of this chapter. 
 
 YIELD OF HopGKINsoN Gop FIELD. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 Year. Alluvial Gold. Stone Crushed. Yield. Total Gold. 
 To end of— Oz. Tons. Oz. Oz. 
 
 S769 ces A at 24,986 Bs 712+ 25,698f 
 INS V rE Pee coe AC: 4,000 13,218 29,818 33,818 
 ise) se iis ee 4,000 25,949 40,435 44,435 
 1879 a... Ar oe 2,021 21,422 31,654 33,675 
 1880... vo ... | (Not estimated) 19,472 25,096 25,096 
 £SS Lee Ans seis 2,941 10,649 12,367 15,308 
 E382 ..; sit eels 928 9,969 11,567 12,495 
 1883 :.. Aa ... | (Not estimated) 8,032 7 203 7,203 
 1884 ... os ... | (Not estimated) 7,750 6,943 6,943 
 ESS Dimi. sek ... | (Not estimated) 5,362 5,553 5,553 
 1886... he ... | (Not estimated) 5,333 4,288 4,288 
 L887 = 5. ce ... | (Not estimated) 2,686 2,399 2,399 
 TS SS vice ane ... | (Not estimated) 2,596 2,325 2,325 
 isso) os.. ae ... | (Not estimated) 2,993 1,960 1,960 
 T8900 sc Pe ... | (Not estimated) 927 1,082 1,082 
 Totals ... as ae 136,508 183,402 222,278 
 
 
 
 + Deduced from figures in Report of the Department of Mines for 1884, p. 11. 
 + Deduced from figures in Report on the Hodgkinson Gold Field. By R.L.J., 1884. 
 
 NORTHCOTE ANTIMONY MINES. 
 
 The three principal antimony lodes, viz., the Emily, Craig’s, and Matilda, occur 
 within the limits of the Hodgkinson Gold Field, nearly in a line running north-west 
 from the head of Leadingham Creek to the head of the Hodgkinson. This line coincides 
 with the strike of the slate and greywacke country-rock, and with the trend of the 
 
 
 
 * Report by R.L.J. on the Chillagoe and Koorboora Mining Districts. Brisbane: by Authority : 1891, 
 
122 
 lodes. The lodes, however, underlie to the south-west, while the strata dip to the north- 
 east. They are traceable for considerable distances on the surface, as quartz reefs 
 stained with antimony oxide, and on being opened show large shoots of solid sulphide 
 of antimony (stibnite). The Emily was worked for some time for gold; the recorded 
 crushings, 382 tons 12 ewt., having yielded 315 oz. 13 dwt. 
 
 The Wardens’ Reports méntion that in 1877 several tons had been prepared for 
 shipment, but as the price in Melbourne was only £12, nothing further had been done; 
 that in 1881, Messrs. Denny and Co. were erecting smelting works; that in 1882, a 
 quantity of ore had been raised; that in 1883, Messrs. Edwin Field and Son had erected 
 large smelting works ; that in 1884, 550 tons of ore had been smelted, yielding 145 tons 
 of crude antimony, valued at £3,500, and that the company had suspended operations ; 
 that in 1885, 70 tons of ore, valued at £300, had been raised; that in 1889, 58 tons, 
 valued at £215, had been raised ; and that in 1890, the Emily Co. had raised and 
 purchased 578 tons 4 ewt., and smelted 571 tons for a yield of 172 tons of crude 
 antimony, and had also forwarded to England 1 ton 4 ewt. 1 qr. of regulus, and 19 tons 
 of oxide (from flues), averaging 70 per cent., and had also forwarded two parcels of 
 7 tons 4 ewt., and 81 tons 5 ewt. of antimony ore from Woodville North (down the 
 Hodgkinson below Thornborough). The value of the yield for the year is estimated at 
 £4,816. 
 
 MULGRAVE GOLD FIELD. 
 
 The Mulgrave River has evidently at one time entered the sea in Trinity Bay, 
 but has been deflected—probably by the flows of basalt which fill up its valley down to 
 the point where it turns sharply round to the south to flow into the sea at Port 
 Constantine. It is a magnificent river, and drains the north side of Mount Bartle 
 Frere, the eastern edge of the Barron Tableland, both sides of the Bellenden-Ker 
 Ranges, and the western slopes of the Malbon-Thompson Range. The Lower Camp, 
 or Goldsborough, is on the left bank of the river, at its junction with Toohey Creek. 
 The Upper Camp is about six miles south of Goldsborough, on the spur dividing Toohey 
 Creek and the Mulgrave. The walls of the Mulgrave Valley are mainly of greywacke, 
 slate, and quartzite ; but between the Lower and Upper Camps flows of basalt fill up 
 the lower portions of the Mulgrave and Toohey Creek Valleys. In following the track 
 from the Upper Camp to Herberton the stratified rocks continue to the edge of the 
 basaltic tableland of the Barron. The Fisheries track from the Mulgrave to 
 Herberton, on the other hand, makes its ascent to the edge of the basalt tableland over 
 granitic rocks. There are evidently two distinct periods of basaltic outflows ; the first, 
 that which “levelled up” the Barron Tableland, and the second, that which choked up, 
 at least for a time, the Mulgrave and other valleys, which had been carved out of the 
 tableland. 
 
 A good deal of gold has been got in the alluvia of the Mulgrave at and below 
 Goldsborough, but no accurate statistics are now obtainable. No serious attempt has 
 as yet been made to search for gold beneath the newer basalt. The same may be said in 
 this locality of the older basalt of the tableland, although the latter is continuous with 
 
 the basaltic flows of the Upper Russell, beneath which payable drifts have been recently 
 discovered. 
 
 At the Lower Camp are the Alice Reef, underlying to south-south-east at 70° 
 (coincident with the bedding of the slates and greywackes), and the Cairns Co-operative 
 Co.’s Reef, vertical and running west-south-west. At the Upper Camp are the 
 Homeward Bound, Orient, Mowbray, Mabel, Scandinavian, and others. The reefs 
 resemble in many points those of the Hodgeinean and, although they cover only a 
 limited area, some of them are likely to prove rich. 
 

 
 
 
 123 
 
 The following information regarding the yield of the Mulgrave is all that ean 
 be extracted from the Wardens’ Reports, which are evidently imperfect, especially as 
 regards alluvial gold obtained in the early days of the field. 
 
 YIELD oF MuLnGRAVE Goup FIeEtp. 
 
 
 
 
 
 
 
 
 
 Year. Quartz Crushed. Tl la Total Gold. 
 Tons. Oz. Oz. 
 1879) © o. bat a os (No crushings) re 440 
 SSO ne. Pe ae ee (No crushings) ses 1,122 
 ADSL 9, - ae Sn (No crushings) re 784 
 L882: aa a ae 442 446 502 
 PL OSSaN esc fs 500 aot 174 302 302 
 1884... bas aK a 29 230 302 
 T8855 cc. aan ae E 222 260 275 
 WSSO5 vs a one ah 100 262 262 
 1888... a og on 115 327 327 
 1889 —-... fis fi re (No crushings) oe 5s 
 1890... ie Ls ... | (Little work done) 
 Total ... =e 4,316 
 
 
 
 
 
 
 
 
 
 PALMER GOLD FIELD. 
 
 The Palmer Gold Field, so far as it has been hitherto opened up, occupies an 
 area which may be roughly estimated at 2,300 square miles. This estimate, as in all 
 other cases, has no relation to the area of the proclaimed goldfield. The greater 
 part of the goldfield is occupied by shales and sandstones in strata, which are tilted up 
 so as to strike from north and south to north-north-west and south-south-east, nearly 
 vertical, but dipping slightly to west and west-south-west. Associated with the sand- 
 stones and shales, and obviously part of the same series, is a belt of limestone, traceable 
 from four miles north of Palmerville southward to the Mitchell River. These stratified 
 rocks have not suffered any appreciable degree of metamorphism ; but owing to lateral 
 pressure the shales have occasionally been cleaved so as to become true slates. They 
 are traversed by dykes of igneous rocks (dolerite and diorite) of much later date. 
 Regarding the age of the stratified rocks, no direct evidence has yet been discovered, 
 the shales and sandstones having yielded only undistinguishable plant-remains, and the 
 limestones only traces of Encrinites and Corals of indeterminable genera. From the 
 lithological resemblance of some of the beds, however, to others found in the 
 Hodgkinson Gold Field, it may be inferred that the Paimer rocks are identical with 
 those of the Hodgkinson—i.e., they belong to the Gympie Formation. 
 
 Nearly 92 per cent. of the gold hitherto obtained from the Palmer has been 
 alluvial gold. The reefs in the neighbourhood of Maytown generally strike west-north- 
 west and north-north-west, and underlie toward the south and west. Those at Lime- 
 stone may be arranged in three groups—the first, running north and south and 
 underlying to the west; the second, east and west, and underlying to the north; 
 the third, north-east and south-west, some underlying north-west and some south- 
 east. The Normanby group of reefs follows no definite rule in their bearing and 
 underlie. 
 
 As will be seen from the following table, the reefs have yielded, from 1874 to 
 1890 inclusive, 105,548 oz. of gold, 
 
 The yield from this source reached its maximum in 1876, the third year of work- 
 ing. This was owing, in the first place, to the ease with which gold could be extracted 
 
124. 
 
 from the surface stone, and in the second place to the comparatively large number of 
 European miners then on the field, who had been originally attracted by the alluvial 
 diggings. The reefs, however, at present show signs of increased activity and pro- 
 ductiveness, 
 
 The production of alluvial gold reached its maximum in 1875, the third year of 
 the existence of the field. The bulk of the total output of 1,210,598 oz. of alluvial 
 gold from 1873 to 1890 has, unfortunately, been reaped by Chinese. 
 
 North of the Palmer River the auriferous rocks are covered by a horizontal cake 
 of the Desert Sandstone (Upper Cretaceous). This Desert Sandstone, there are cogent 
 geological reasons for believing, may cover extensive deep leads of concentrated 
 auriferous wash, which may yet prove even richer than the old alluvial diggings of the 
 Palmer. It may be mentioned that the alluvial gold in many cases is found in localities 
 where it is impossible to believe that it ean have come from local reefs; and everything 
 points to the old land-surface now covered by the Desert Sandstone as its original 
 source. (See Chapter on Desert Sandstone.) 
 
 YIELD oF PALMER GoLp FIELD. 
 
 
 
 
 
 
 
 Year. Alluvial Gold. Reef Gold. Total. 
 Oz. Tons Quartz. Oz. Oz. 
 
 *1873 nat hate ae 58,829 ae aie 58,829 
 1874 a sir siete 150,000 ime 200 150,200 
 1875 ate mee eis 250,000 ee 400 250,400 
 1876 wae sats ind 185,000 4,766 15,000 200,000 
 1877 Nee dee Ber 167,760 4,949 11,811 179,571 
 1878 te ane eae 112,000 4,061 8,283 120,233 
 1879 wae Ae ae 79,998 4,814. 10,002 90,000 
 1880 ane sae Sa 58,513 3,016 6,920 65,433 
 1881 AR das Beis 45,171 3,170 6,789 51,960 
 1882 nea ana Bae 33,092 2,704, 4,247 37,339 
 1883 as Ose ae PAs bya 2,702 2,918 24,089 
 1884 ee oe és 13,764 1,902 1,873 15,637 
 1885 a \ 8 9,960 1,676 2,953 12,913 
 1886 ae ae ae 6,521 1,101 2,066 8,587 
 1887 ache sss eer 5,000 1,477 1,981 6,981 
 1888 me ane Ves 5,692 2,216 10,732 16,424 
 1889 a fee Ane 4,298 3,079 12,563 16,861 
 1890 ee ee 3,829 5,675 6,860 10,689 
 Grand totals ... ane 1,210,598 47,308 105,548 1,316,146 
 
 
 
 
 
 
 
 
 
 
 
 * Deduced from data in Report of Department of Mines for 1884, p, 10. 
 
 CANNIBAL CREEK TIN FIELD. 
 
 Up to 31st December, 1884, 2,373 tons of tin ore, valued at £102,300 10s., had 
 been exported from the Palmer Gold Field, chiefly from alluvial workings on Granite 
 and Cannibal Creeks. Although this stream tin was collected from slate and greywacke 
 country, and in the neighbourhood of the Cannibal Creek lodes, it probably came, for 
 the most part, from the granite range to the east. This range, which is a stronghold of 
 the Aborigines, has never been sufficiently prospected for lodes. The lodes on Cannibal 
 Creek are large quartz reefs, running EH. 15° S., through a country-rock of slate and 
 greywacke, and containing some tin ore. The formation of a company to work these 
 lodes resulted disastrously, as expensive machinery was erected before the mines were 
 proved to be payable. ’ 
 
-—* 
 
 ae 
 
 
 
 125 
 
 YIELD OF PALMER TIN FIELD. 
 
 
 
 
 
 Tons. Estimated value. 
 Lis: 
 (Prior to) 1880* Ae ase ... 450 AY) es a9a 22,500 O 
 1880 art 80 sce WSS) tie mG mae 38,000 O 
 1881+ a aa vas =D Htc Hoe oe 16,847 10 
 1882 fie hs m,- FOCUS. . bse Bc 11,340 0 
 1883f ee ee se LSI) sre res eee 10,119 O 
 1884, et ae Pi athe A00 a8 oor 3,556 O 
 Totals ne d6c 1s 25018 nee naa ... £102,300 10 
 
 * Exported by Whitehead and Co. 
 + Including, for the first time, Cannibal Creek lode-tin. 
 t Cannibal Creek Company wound up. 
 
 MITCHELL ANTIMONY MINES. 
 
 Information has recently been received to the effect that very important dis- 
 coveries of auriferous antimony ore have been made by Mr. J. V. Mulligan and others, 
 on the Mitchell River near the Limestone Gold Mines. 
 
 MOUNT ALBION SILVER FIELD. 
 
 West of the stanniferous porphyritic and granitic country of Herberton and 
 Watsonville, a band of stratified rocks stretches north-westward from the head of the 
 Dry River. They consist, for the most part, of shales and siliceous grits, the latter 
 occasionally altered so as to be almost quartzites. Their general strike appears to be 
 from north and south to north-north-west and south-south-east, but at Mount Albion 
 itself, which is the most highly mineralised portion of the district, the rocks (among 
 which siliceous grits predominate) have been minced up by innumerable faults into 
 small segments, in each of which the strata have their own peculiar dip. In the Mount 
 Albion Mine some sandstones are marked with reed-like plant-impressions, but nothing 
 has yet been discovered sufficiently distinct to afford any positive evidence as to the 
 age of the deposits. 
 
 In the principal mines on Mount Albion—viz., the Albion, Lady Jane, and 
 Barossa—immense deposits of ore occur in a very irregular manner. It appears that 
 the faults are even more numerous than the evidence observable at the surface would 
 indicate, and that the ore has filled up fissures formed by faults which intersect one 
 another in every direction, so that there are no definite walls which can be followed for 
 any distance. The ores are earthy and ferruginous, with argentiferous lead oxides and 
 carbonates, and probably a good deal of silver chloride in fine particles accounts for 
 their occasional extraordinary richness (600 or 700 oz. of silver to the ton). Large 
 “slugs”? of horn silver are met with from time to time in the workings. In the 
 Albion some were obtained at the surface and at the depth of nineteen feet. In the 
 Lady Jane some were obtained at the one hundred and thirty and one hundred and 
 eighty feet levels. The mines have not yet reached the water level, which is probably 
 low, the mount being well drained by the faults which intersect it in every direction. 
 Tron and lead oxides and carbonates, therefore, predominate, sulphide and sulphate 
 ores forming, except in the Barossa (where the galena is associated with zinc-blende), 
 only a small proportion of the ore. 
 
 In marked contrast to the deposits of ore on Mount Albion are those which 
 occur about a mile and a-half to the south-east. A large lode, the Silverhill, which 
 might be taken as a typical example of what is meant by a true fissure lode, runs north 
 and south through slate country, underlying at 45° to W. It is distinctly traceable 
 
126 
 
 across two hills and two gullies, for a distance of 1,500 feet, by occasional exposures 
 of galena. In the workings the galena ore runs from nine inches to three feet in 
 thickness, is occasionally associated with anglesite, zinc-blende, and pyrites, and is 
 accompanied by a brecciform gangue of broken country-rock. The ore, although more 
 than payable, is not nearly so rich in silver as that of Mount Albion. The mines at 
 the Orient Camp, six miles north-east of Mount Albion, produce a similar class of ore to 
 that of Silverhill. 
 
 Smelting works have been erected on Cummings Creek, Mount Albion, by 
 Messrs. John Moffatt and Co., and the ores have been very successfully treated. The 
 earthy ores of Mount Albion are mixed in due proportions with the galena ores of the 
 Orient and Silverhill, and with ironstone and limestone from the Dry River. The 
 bullion is cast into ingots of lead containing generally about 600 oz. of silver to the 
 ton, and exported in this form. 
 
 Some confusion has arisen, owing to the Mineral Lands Commissioner having 
 given in 1885 the amount of ore raised, while in 1886 only the amount smelted is given. | 
 Probably the amount smelted in the latter year included some of that raised in the 
 former, so that the returns are defective for statistical purposes. The following notes 
 embody all the information obtainable :—In 1885, 2,028 tons of ore were raised, con- 
 taining 218,450 oz. of silver. Estimating the value of the ore on a basis of 3s. 6d. per 
 oz. of silver, the value would be £38,229. In 1886, 1,4403 tons of ore smelted, yielded 
 223 tons of bullion, estimated to contain 88,224 oz. of silver; at 3s. 6d. per oz. of silver, 
 the value would be £15,439: 340 tons of ore, valued at £22,446, are said to have been 
 raised during the year. In 1887, 4,849 tons of ore were smelted, yielding 1,041 tons of 
 builion, estimated to contain 272,863 oz. of silver, and valued at £54,572 12s. How 
 much was raised during the year is not stated.* In 1888, 5,347 tons of ore were smelted, 
 yielding 1,083 tons of bullion, estimated to contain 229,308 oz. of silver, and valued at 
 £42,000. In 1889, 5,801 tons of ore were smelted, yielding 896 tons of bullion, 
 estimated to contain 221,374 oz. of silver, valued at £55,683, besides 527 tons of 
 sulphide ore exported to England for treatment, estimated to contain 96,818 oz. of 
 silver. In 1890, 4,017 tons smelted, yielding 888 tons of bullion, estimated to contain 
 155,000 oz. of silver; besides 425 tons of sulphide ore exported, estimated to contain 
 65,621 oz. of silver; and 128 tons of ore forwarded to Aldershot, estimated to contain 
 10,368 oz. of silver. 
 
 These total values, for obvious reasons, cannot be added together. 
 
 BRY RIVER SILVER FIELD. 
 
 This field lies in the belt of mineralised stratified rocks which extends south- 
 eastward from Mount Albion. The slates and greywackes which form the mass of the 
 strata strike mainly north and south. The principal lodes—the Try-no-More, Dunn’s, 
 Silver Streak, Target, Silver Valley, White Star, and Rainbow—trend on an average 
 from north-west to south-east, and underlie to the south-west. They have, as a rule, 
 caps of ferruginous gossan showing lead oxide, galena, sulphate of lead, and carbonate 
 of copper. In the Try-no-More, the ore at a greater depth is somewhat complex, being 
 composed of copper pyrites, grey iron pyrites, galena, and zinc-blende. The other mines, 
 however, yield chiefly argentiferous galena, with occasional zine-blende. A smelting 
 company commenced operations in 1883, and suspended operations in 1886. There is 
 no doubt that several of the mines are distinctly payable. The failure of the field is 
 
 
 
 
 
 * Except in Table A, where 1,041 tons and £54,572 are given, evidently by mistake, as the amount 
 of ore raised and its value, 
 
a | ae 
 
 
 
 127 
 
 attributed locally to the policy of the smelting company, which was said to have been 
 to force outside holders to sell their mines. The result is said to have been that 
 ultimately these mines ceased to produce enough to keep the works employed. A 
 decidedly good opening is offered by this field for a smelting work conducted on a more 
 rational principle. There is a prospect of the smelting works being again set going, 
 and several of the mines have recently been reopened. 
 For some years operations on the field were limited to the raising of limestone 
 and ironstone, used as fluxes at the Mount Albion Works. 
 The following table gives extracts from the Mineral Lands Commissioner's 
 Reports :— 
 Yiretp oF Dry River Sitver FIevp. 
 1883.—100 tons ore smelted yielded 18} tons bullion, valued at £832. 
 1884.—200 tons ore raised, valued at £1,600. 
 1885.—500 tons ore raised, and dressed for smelting; estimated silver 
 contents, 30,000 oz. ; estimated value, £5,844. 
 (“The Pacific Smelter had a trial run, and smelted 120 tons of ore for a 
 yield of 42 tons of bullion, valued at £40 per ton; but smelting has again 
 been suspended.”’) A 
 1886.—420 tons ore smelted yielded 117 tons bullion; estimated silver 
 contents, 22,230 oz.; estimated value, £4,668. (“But at present 
 smelting operations are suspended.’’) 
 
 NEBO (MOUNT BRITTON) GOLD FIELD. 
 
 The reefs of the Mount Britton Gold Field occur partly in diorite and partly in 
 grey and black shales and sandstones. The stratified rocks, which contain indistinct 
 plant-remains, probably belong to the Gympie Formation, and the igneous rocks appear 
 to be partly interbedded and partly intrusive. The field was opened in 1881 as an 
 alluvial diggings, and has yielded some large nuggets—69 oz., 50 oz., 45 oz., 40 oz, and 
 35 0z.—with but a small proportion of fine gold. Two groups of reefs, one at the head 
 of Nuggetty Gully and the other about three-quarters of a mile to the south, have 
 yielded some rich crushings. Except the totals for the different years, no returns have 
 been furnished by the Wardens. In the latter half of 1888, the Little Wanderer Reef 
 crushed 421 tons of stone for 2,4160z. of gold. <A third group of reefs, near Mount 
 Clarke, looks as if it might yet prove valuable. 
 
 YIELD oF Mount Britton Goxup FIe Lp. 
 
 
 
 
 
 
 
 
 
 
 
 REEF GOLD. 
 Year. * Alluvial Gold. Total Gold. 
 Stone Crushed. Gold therefrom. 
 Oz. Tons. Oz. Oz. 
 1881 O80 50 se 4,808 (No crushings) sir 4,808 
 1882 ae 500 ei 625 ? 627 2,779 3,404 
 1883 oe ar nea 520 P 686 2,095 2,615 
 1884, Said eee ia 800 ? 200 500 1,300 
 1885 on ae se Bee (No returns) ee es 
 1886 206 cee sc say, 300 = say, 50 350 
 1887 pad oo big 450 12 16 466 
 1888 ie ae ‘ot 268 wae 489 UOT 
 1889 “me ane sas 68 28 94 162 
 1890 aad ae Age 95 22 34 129 
 Total os ne Mee fy vid 13,991 
 
 
 
 
 
128 
 
 SELLHEIM SILVER FIELD. 
 
 The majority of the argentiferous galena lodes of the Sellheim occur in an 
 altered dolerite rock,* which appears to have intruded among and spread over the 
 denuded surfaces of a series of stratified rocks. A few of the lodes have been worked 
 to a limited extent in the latter. The stratified rocks in question are best seen in 
 Gordon Gully, which falls into the left bank of the Sellheim River, south of Euka- 
 lunda township. They have a general dip to S.W. at angles varying from 20° to 
 30°, and consist of bluish-grey shales and fine-grained sandstones, marked with faint 
 impressions of fossils, among which I could detect Spirifera, Productus, Pecten or 
 Aviculopecten, and Stenopora. Although the fossils obtained were all very imperfect, 
 I have little hesitation in classing the strata in which they occur with the Gympie Beds. 
 This series appears to be faulted on the east against granite and on the west against 
 the Star Beds already described. It is in this neighbourhood that the Chonetes, &c., 
 beds, referred to by Daintree and McCoy, occur. 
 
 The field is minutely described in a Report by the Writer. The principal 
 lines of lode are the Pyramid, Bonnie Dundee, General Gordon, and Rob Roy, some 
 of them over half-a-mile in length. No smelting works have yet been erected, and, 
 considering the expense of carriage of the ore to Bowen, it speaks well for the field 
 that it has lived so long. 
 
 Bismuth mines (see Chapter II.) occur in the neighbourhood, but in granite or 
 syenite country. | 
 
 YIELD OF SELLHEIM SILVER MINEs. 
 
 
 
 Ore Exported. Value. 
 Tons. £ 
 
 1883 ABE aaC =e 20 don 400 
 1884 4c see a, Add) St 2,400 
 1885 So sie eS as 5,165 
 1886 See a nae 743, Bad 5,150 
 1887 ce ae bees FAUT an 4,215 
 1888 ee re .. ~=480 ree 8,061 
 1889 eae ae Sate © ABP ae 2,462 
 * Totals a ... 1,446 ae 27,853 
 
 *The return of silver for 1890 cannot be given, as the Commissioner's Report only gives the total of silver and 
 bismuth ore as 53 tons 11 ewt., valued at £1,709 Os. 6d, 
 
 J. 
 
 
 
 * See Mr. Clarke’s Petrographical Notes. 
 + Report on the Sellheim Silver Mines and Surrounding District. Brisbane: by Authority: 1889, 
 
CHAPTER X. 
 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 THE STAR FORMATION. 
 
 Tre Star Basin forms an area of about thirty-six square miles, at the junction of the 
 Great and Little Star Rivers, which are tributaries of the Upper Burdekin. Disposed 
 with only a gentle dip, and consisting of unaltered stratified rocks, it contrasts in a 
 striking manner with the surrounding granites, gneisses, slates, and schists. The 
 latter, occurring between the Star and Keelbottom Rivers, and forming the country- 
 rock of the Star Gold Field, and of the now much better known Silver Field of 
 Argentine, as well as the stanniferous porphyry of Running Creek, are of much older 
 date than the rocks which I named, in 1878, the ‘‘Star Beds,’ and which I then 
 regarded (following Messrs. Daintree and R. Etheridge, F.R.S.) as Upper Devonian. 
 
 In a hill about three and a-half miles south-south-east of the Star Station. a 
 number of beds of coarse hard siliceous sandstone or grit, with quartz pebbles, rest 
 on granite and dip to W. at an angle of 12°, presenting to the east an escarpment 
 which rises some two hundred feet above the level of the granite. The same beds are 
 seen in Horse Creek. Their total thickness cannot be less than three hundred feet. 
 
 On Dinner Creek, the beds which are seen in closest proximity are coarse grits 
 and conglomerates, with pebbles of quartz and lydian-stone. Although these strata 
 are probably on the same horizon as the grits of the hill referred to in the last paragraph, 
 they dip at 20° towards the position where the metamorphic rocks appear at the surface. 
 There is probably, therefore, a fault between the two formations at this place. 
 
 Where the Little Star River enters the Basin from the north, the lowest of the 
 Star Beds open to observation are coarse gritty sandstones, containing a few pebbles 
 and dipping to S. at an angle of 30°. 
 
 On the west side of the Great Star River, where the grits at the base of the 
 series might have been expected to reappear at the surface, they were not observed. It 
 is quite possible that they may have thinned out in the six miles that intervene. 
 
 Supposing the dip of 12° to continue without interruption from the grit of the 
 hill down the course of Horse Creek, a series of strata equal to a vertical thickness of 
 eight hundred feet should intervene between the grit and the strata next exposed to view, 
 viz., about twenty feet of bluish shales, somewhat calcareous, which dip to S8.E. at 20°, 
 on the western branch of Sandy Creek near an old grave. The shales are covered with 
 impressions of Lepidodendron. Similar shales, also rich in Lepidodendron-impressions, 
 are met with on the eastern branch of the creek, where they are turned up on-end. In 
 this locality a fault probably divides the outcrop of the metamorphic slates, &c., from 
 the Star Beds, concealing the lowest members of the latter series. 
 
 Next in ascending order, after a gap, estimated at thirty-five feet, is a bed of 
 sandstone dipping to the south, and about ten feet in thickness, seen at the mouth of 
 Sandy Creek. Above the sandstone, where Corner Creek falls into the Great Star 
 River, are about twelve feet of green shales dipping at 30° to S.S.W. These shales are 
 exceedingly rich in organic remains, among which the following have been recognised :— 
 
 Lepidodendron australe, McCoy. 
 Fe veltheimianum, Sternb. 
 Actinocrinus, sp. ind., Pl. 7, fig. 9. 
 
180 
 
 Beyrichia varicosa, T. R. Jones, Pl. 7, fig. 15. 
 Phillipsia dubia, Eth. 
 Fenestella multiporata, De Kon. 
 Spirifera bicarinata, Eth. fil., Pl. 10, figs. 9, 13; Pl. 37, fig. 17; Pl. 11, 
 figs. 1-3. 
 Spiriferina, sp. ind. 
 Reticularia Urei, Fleming. 
 Retzia radialis, Phill. 
 Orthis resupinata, Martin. 
 Strophomena rhomboidaiis, var. analoga, Phill. 
 Chonetes cracowensis, Eth. 
 4 sp. ind. (a), Pl. 18, fig. 10; Pl. 37, figs. 21, 22. 
 Entolium, sp. 
 Euchondria, sp. 
 Nuculana, sp. ind. 
 Naticopsis variata, Phill. ? 
 a sp. tnd. 
 Porcellia Pearsi, Eth. fil., Pi. 15, figs. 7, 8. 
 Orthoceras, sp. 
 
 A gap of thirty-five feet intervenes between the fossiliferous beds of Corner 
 Creek and the next succeeding, which is seen in Brock’s Creek, viz., a bed of blue 
 crystalline limestone at least twelve feet in thickness. Thin sections of the limestone, 
 examined under the microscope, revealed no traces of organic remains. 
 
 About fifty yards further down Brock’s Creek, and probably about ten feet above 
 the last-mentioned limestone, are fifteen feet of hard yeliow sandstones, among which 
 there are some greenish calcareous bands, and hard shales, dipping to S. at 25° to 30°. 
 In this section I observed a curious case of contortion in the upper beds not continued 
 into the lower beds (see Plate 53, fig. 3). This local contortion I ascribe to the unequal 
 contraction of the purely sedimentary sandstones and shales and the partly chemically- 
 formed calcareous sandstone. 
 
 After a gap, probably not amounting to more than fifteen feet, the following 
 section is seen in Donald’s Creek, dipping to S. at 20° :— 
 
 Teet 
 Blue shales with ironstone nodules, and impressions of Lepidodendron 
 australe (McCoy), and thin hard limestone bands (upper beds at 
 mouth of creek) ... Pact rey ae a aoe ine Bre te $) 
 Impure blue limestone ... bts iP ah ee +f Ses ae) 
 Shales... re G ss ie a Sa i we cen LO 
 Hard sandstone .., s a cork aL 
 Alternate bands of shale Aa fue hard Palcarsoue ete the sand- 
 stone bands containing shells, and the shales plant-remains ... rel 
 Hard sandstones and shales is : Ae Ses mek ar) 
 Confused section, shales seen at intervals—1o0m for va ee i LOG. 
 Fine dark-blue limestone or cement-stone, with conchoidal fracture, in 
 three beds... 5 a an ae 
 Shales and hard sandstone, with bale OW see 20 
 Hard greenish sandstone (weathering spheroidally in parts) with 
 Lepidodendron — oe el Sy, ra ¥e ree eo!) 
 371 
 
 A bed of coarse conglomerate, twenty-five feet in thickness, seen in the Little 
 Star River, north of the ford on the Coppermine Road, succeeds the uppermost beds 
 
131 
 
 in the above section, a gap of probably about thirty-five feet intervening. The con- 
 glomerate is traceable on the surface for a mile and a-half. A band of porphyry, 
 probably intrusive, although it follows the line of strike of the sedimentary beds, is 
 seen in contact with the conglomerate in the Little Star River a few hundred yards 
 above the ford. 
 
 A gap of about thirty feet is supposed to separate the last-mentioned con- 
 glomerate from the next higher bed, viz., a coarsely crystalline limestone, about one foot 
 in thickness, seen in Horse Creek, and showing on its weathered surface sections of 
 shells (Orthis, &c.), Enecrinites, and Corals. A microscopic examination of the limestone 
 matrix in which the larger fossils are preserved proved it to be a mass of foraminifera. 
 The forms of the larger shells are perfect, but their substance has been entirely replaced 
 by calespar.. Above this limestone lie about twenty feet of thin-bedded calcareous 
 sandstones and shales, dipping. to W. at 30°, and containing Orthis, Chonetes, and 
 Gasteropods, together with Lepidodendron australe, McCoy. ‘To these succeed twenty 
 feet of shales and hard dark-blue sandstone, dipping to the south-east; also seen in 
 Horse Creek, south of the Station Paddock. 
 
 Next in ascending order, after a gap of about twenty feet, is a coarse con- 
 glomerate of coarse pebbles, dipping at 60° to N.W., fifteen feet in thickness, seen 
 in the Little Star River at the mouth of Horse Creek. Above this are about twenty 
 feet of green shales and fine hard caleareous sandstones, seen in the Little River at 
 the ford on the Coppermine road. 
 
 As no other area in the Star Beds has as yet been mapped in the like detail, the 
 strata above described are thrown into tabular form for convenience in future 
 comparisons. 
 
 Feet. 
 Green shales and fine hard calcareous sandstones—Little River at 
 ford on Coppermine Road Lee a ot 20 
 Coarse conglomerate—Little Star River, at meatls of Hor se Croek a 15 
 Caps ts 20 
 Shales and had) dark- blue sandatones=“Horse Cr eck, mete of Station 
 ; Paddock ... : 20 
 328 Thin-bedded calcareous sandstones and ‘shales, eontainine Or this: 
 SEe3 Chonetes, Gasteropods, and Lepidodendron australe ae me 20 
 gs #8 Limestone, with shells, encrinites, and corals... ae ane a i 
 Gap... 4 30 
 Coarse conglomerate—Little Star River, north of ford o: on Goppermine 
 Road re 1 if a. ei a i: me oe 25 
 ap! :.. 35 
 ( Blue shales, with ironstone nodules andi; pepressions of Pe odentias on 
 australe, McCoy, and thin hard limestone bands {upper beds, at 
 mouth of creek) .. ee ae ny ef oes sae oe 80 
 Impure blue limestone oi ne so aH is Hee as 2 
 . | Shales ... A rec e ty i ee hie Hes cs 15 
 3 Hard sandstone a 1 
 ¢ | Alternate bands of shales and fine hard calcareous ssaateeae: ie 
 Ag sandstone bands containing shells, and the shales plant-remains... 50 
 = Hard sandstones and shales .. a ae Ex: an 70 
 & | Confused section, shales seen at Bete ee oroory for aS ee a LOO 
 © | Fine dark-blue limestone or cement- stone, with conchoidal feateave 
 —in three beds ... Ay fea ae oe 3 
 Shales and hard sandstone with feet bbetes Phe Bie sete aa 20 
 
 Hard greenish sandstone (weathering spheroidally in ach with 
 L eodondeon ae ee a +f one ta x, a 30 
 
1382 
 
 Feet. 
 
 Hard yellow sandstones, with greenish calcareous bands and hard 
 shales—Brock’s Creek ... a i. Lo af ar: ia 15 
 Gap... coe ae vee a Bhs ae Th es ia 10 
 Blue limestone—Brock’s Creek ... & Re = +f ak 12 
 Gap ee ¥h a a oa 5s fee eas ess 35 
 Green shales, fossiliferous—Corner Creek Aa one nee e 12 
 Sandstone—mouth of Sandy Creek ae 0 a ees ee 10 
 
 Bluish calcareous shales, with Lepidodendron—west branch of Sandy 
 Creek - ref oe ae cae fie a ae oa 20 
 
 Grits and conglomerates—Horse Creek and hill to south, Dinner 
 Creek and Little Star River... me ais tf s ... 300 
 Total a ae ae Pepene Beire, 
 
 White sandstones, pebbly grits, and conglomerates of considerable thickness, 
 belonging to the Star Beds, overlie the mica-schists and slates of the Argentine Silver 
 Field. They are inclined at comparatively low angles, and form cappings on the higher 
 hills of the district such as Camp Hill, Ben Lomond, and the hill lying between the 
 Bonanza and Caroline Mines.* The section (Pl. 54, fig. 1) shows the relations of the 
 sandstones, &c., overlying the silverfield to the Star Beds, as developed in the type 
 district, and to the underlying rocks. It will be observed that the Star Beds some- 
 times overlie the slates and schists of the silverfield, and sometimes rest directly on 
 granite. 
 
 In my Handbook of Queensland Geology,+ I described, under the name 
 of the “ Dotswood Beds,” a series of strata largely developed in the valleys 
 of the Fanning and Keelbottom, which I then believed to succeed the Fanning 
 (Burdekin) Limestone (Middle Devonian), conformably. ‘To this horizon I referred 
 the plant Dicranophyllum australicum, Dawson, occurring in a bed of sandstone 
 immediately, and conformably, overlying the Fanning Limestone. I have since, as 
 already stated, ascertained that the Fanning and Burdekin Limestones are succeeded by 
 a great thickness of strata belonging to the same period (Middle Devonian), to which I 
 have therefore relegated the plant in question. Moreover, I have since found in the 
 “‘ Dotswood Beds,” as originally described, an abundant series of fossils which leave no 
 doubt that the “ Dotswood Beds” are identical with the “Star Beds,” or at least are 
 part and parcel of the same formation. 
 
 In Keelbottom Valley, near Dotswood, the strata of the so-called “ Dotswood 
 Beds”’ dip to E. at 30°, and form a series of ridges across the valley. Taking into 
 account the high dip and the extent of ground oecupied by the outcrop of the strata, 
 they must be some thousands of feet in thickness. Beds of brown felspathic sandstone 
 alternate with conglomerates and red shales which are marked conspicuously with white 
 spots. The conglomerates contain pebbles, up to six inches in diameter, the majority of 
 which are of pink porphyry, a few being of hardened white sandstone or quartzite. 
 The porphyry pebbles, as well as the felspathic sandstones and the gritty felspathic 
 matrix of the conglomerates, clearly prove that the deposit was derived, as a whole, 
 from the waste of voleanic or metamorphic materials, It bears a striking resemblance 
 to the Lower Old Red of Perthshire, Scotland. 
 
 
 
 
 
 * See Map attached to Report by R.L.J, on the Argentine (Star) Silver Mines, Brisbane: by 
 Authority : 1886. 
 + Brisbane : 1886, 
 
133 
 
 On the left bank of the Burdekin, opposite Dalrymple, the strata are of a 
 character essentially similar to those of Dotswood. They consist of reddish and 
 chocolate-coloured sandstones, which are often cross-bedded, and sometimes flaggy, with 
 faint ripple-marks. In places they enclose little pellets of chocolate-coloured shale. 
 Buff ferruginous spets are common in the interior of the sandstone. The shales are 
 occasionally greenish, but the red and chocolate-coloured beds predominate. The 
 red and chocolate-coloured shales are dotted with white spots, and often weather 
 spheroidally. 
 
 The little hill called Mount Keelbottom consists of a pale pinkish porphyry with 
 a base of acidic felspar, crystal of orthoclase felspar, and water-clear blebs of quarts. 
 The porphyry has a quasi-schistose structure which is specially noticeable on weathered 
 surfaces. The same is observable in the hill immediately opposite Dalrymple, where a 
 series of escarpments coincides in direction with the outcrop of the sandstone beds. It 
 is more than likely that the porphyry is a metamorphosed volcanic tuff, but whether 
 it is interbedded with the sandstone strata, or is of older date, has not been ascer- 
 tained. 
 
 A visit to the Keelbottom River, in June, 1879, enabled me to include in the 
 so-called “ Dotswood” (Star) Beds the greater part of the Keelbottom Valley up to the 
 junction of Speed Creek, and a considerable portion of the hilly region known as 
 Table-top Downs. Leaving the eastward bend of the Keelbottom River, between the 
 Plumtree Inn and Speed Creek, to ascend the hill on the eastern side of the valley, 
 several low ridges are crossed composed of grey, greenish, and brownish sandstones, 
 dipping at about 30° to H.S.E. The sandstones are generally in not very thick beds, 
 are hard and tough, and occasionally weather spheroidally. Some of the brown beds 
 are easily recognisable as having been derived from the waste of the adjacent granite. 
 All the sandstones have a greater or less admixture of felspathic granules with the 
 siliceous. Towards the base of the hill, the sandstones become more conglomeratic than 
 in the valley, the pebbles being of porphyry, quartzite, quartz, and various metamorphic 
 rocks (gneiss, slate, &c.) The steep slope of the hill is of conglomerate. Near the top 
 is a thick, conspicuous stratum of yellow cross-bedded sandstone, capped by amygdaloidal 
 dolerite, about ten feet in thickness. The dolerite is again surmounted by yellow 
 sandstone. The strata, when followed in ascending order at right angles to their 
 outcrops, become gradually more and more mixed up with traphean beds (varying from 
 dolerites to porphyrites), till, towards the Fanning, the intercalated sandstones are 
 scarcely met with. These ancient lava-beds, especially the porphyrites, are cupriferous 
 over a wide area. Large masses of native copper are found in the Keelbottom Copper 
 Mine. 
 
 In 1886 I visited the range on the eastern side of the Keelbottom Valley, 
 north-east of the Old Plumtree Inn (Boolangalla Town Reserve). On ascending 
 from the old inn the slope was found to consist of coarse, white, hard grit and 
 conglomerate, dipping at 40° to S.S.E. These beds are intersected by a sheet of 
 intrusive porphyry which runs obliquely across the bedding. The porphyry forms 
 the top of the mountain, which has a double summit, the two peaks being divided 
 by the head of a gully which falls into the Keelbottom River. Below the scarp 
 formed by the edge of the porphyry are some beds of grit and conglomerate, 
 divided by flaggy beds of fine-grained grey sandstones and beds of shale. The fine- 
 grained sandstones yielded Spirifera bicarinata, Eth. fil.; Rhynchonella pleurodon, 
 Phill.; Ohonetes, sp. ind. (a), Pl. 13, fig. 10, Pl. 37, figs. 21, 22; Ohonetes, sp. ind. 
 (c), Pl. 37, fig. 20, and numerous other fossils common to the Star Beds in the type 
 district. 
 
134 
 
 Mr. A. Gibb Maitland speaks in the following terms * of a series of strata which 
 he refers to the Star Beds :— 
 
 “Tt is with hesitation that I class a series of grits, sandstones, and conglomerates, 
 occurring in the south-east corner of the country, with the Star Beds. No organic 
 remains were detected in any of them. 
 
 “Tt is only their strong lithological resemblance to strata of that age in other 
 areas that gives any clue to their geological position. They do not occupy a very 
 extensive tract of country. 
 
 “The first locality in which these beds were met with is about north-north-east 
 of Kangaroo Hills Station, and distant about eight to ten miles. They consist of coarse 
 whitish quartzose grits and conglomerates, lying almost horizontally and forming 
 conspicuous escarpments, traceable for some distance; they rest alternately upon 
 granite and the upturned edges of a series of hardened grits and shales, which have a 
 general north-east and south-west strike. Sect. IV., plate 1,¢ gives a general idea of 
 their occurrence. Some little distance from Mount fox to the north, about ten feet 
 thick of a whitish quartzose grit resting on granite and dipping at 70° N.E., is seen to 
 be overflown by sheets of basaltic lava. Much lower down the creek boulders of grit 
 were seen, but this is the only section where the rock is met with én situ. The section 
 is shown Sect. I., plate 2. 
 
 ‘An extensive development of these beds is to be seen in the Blue Range, which 
 occupies that piece of country drained by the tributaries of Tomahawk or Packsaddle 
 Creek, Camel Creek, and some minor affluents of the Burdekin. In a traverse from the 
 camp on Tomahawk Creek to the Blue Range the country was found to consist of shales 
 and ferruginous felspathic sandstones or greywackes, in which no fossils were detected. 
 These beds are nearly vertical, and strike north-east and south-west. 
 
 “The sedimentary strata which rest unconformably upon the vertical beds are 
 arranged in the form of a synclinal trough, the longer axis of which appears to trend in 
 a north-westerly direction. Scaling the first cliff formed by the denudation of the Star 
 Beds, the quasi-vitreous white sandstones were found to dip S. at angles of about 35°; 
 the trend of the mural precipice was east-south-east. The actual summit was ascertained 
 by Aneroid to be 2,030 feet above sea-level. This mountain is almost isolated from the 
 main mass of the range by a low saddle 1,620 feet above sea-level, and which divides 
 waters flowing east and west. In this low saddle vertical ferruginous felspathic grits 
 striking north-east and south-west crop out at intervals. After passing over a low 
 table of grit, beneath which the vertical sedimentary beds are seen to lie, a hill 1,930 
 feet above sea-level was ascended and found to be capped with grits, which were seamed 
 in places with veinlets of quartz. At the foot of the hill in the north-east these beds 
 appear to be faulted against the vertical shales and greywackes. ‘The highest point of 
 the range was found to be 2,670 feet in height, and composed of coarse grit and 
 conglomerate, with a vertical wall-like precipice over 100 feet in height facing the south- 
 west. (Section IT., plate 2.) | 
 
 “From this point the general character of the range could be well seen, and its 
 geological structure. Owing to darkness coming on, I was unable to visit the south- 
 westerly end of the synclinal trough. 
 
 ‘“‘ Another minor area of what are regarded as representatives of the Star Beds 
 is met with in the vicinity of Lake Lucy Station. Some distance west from the head 
 station a conspicuous low hill is seen to be composed of a semi-vitreous white grit or 
 quartzite, which appears to unconformably overlie the Wairuna Beds. 
 
 * Report on the Geology and Mineral Resources of the Upper Burdekin. Brisbane: by Authority: 1891. 
 + Of Mr, Maitland’s Report 
 

 
 135 
 
 “A gully flowing south-west from the divide, east-south-east of the station, and 
 about three miles distant from it, another section showing a similar grit or quartzite is 
 seen in a cliff which trends north-east and south-west.” 
 
 Near the mouths of the Cape, Suttor, and Sellheim Rivers, a considerable area is 
 occupied by the Star Beds, which cover the greater part of Harvest Home, Lornesleigh, 
 and Mount McConnell Runs. They rest at their northern boundary on granite, and at 
 their southern boundary, near the Sellheim Silver Mines, they are apparently separated 
 by a fault from the Gympie Beds. They appear to be disposed in a basin, the synclinal 
 axis of which is a short distance south of Mount McConnell Station. Near the 
 silver-mines they dip to N.W. at angles varying from 40° to 50°. On the northern 
 boundary, near Mount McConnell, the lowest beds seen, which form what are known 
 as the Devil’s Crags, are white sandstones, hardened but otherwise not much 
 altered, dipping at 75° to E.15° S. The sandstone resembles lithologically those of 
 the Star Beds near Dotswood. Between the Crags and Mount McConnell Station 
 occasional outcrops’ of stratified rocks, including quartzites, greywackes, flagg) 
 sandstones, and shales, are met with, dipping at 40° to S.S.E. The quartzites 
 have small dark flakes of carbonaceous matter. The greywackes, which are often 
 caleareous, are full of lines of small holes, but I could see no distinet moulds of 
 organic remains. On the road from Mount McConnell Station to Lornesleigh, 
 three miles west of the former, I saw a felspathic sandstone full of stems of 
 Lepidodendron, and another stem covered with circular leaf-scars (Cyclostigma ?). 
 Similar fossils, I am informed, are obtained at Lornesleigh and Harvest Home. 
 Lepidodendron australe, McCoy, has been obtained at Harvest Home by Mr. P. W. 
 Pears.* 
 
 In Conrad’s Dorf Block, about four miles south-east of Mount McConnell 
 Station, sandstones and shales with plant-remains, including Cyclostigma (?), dip to 
 N.W. at over 45°. About two miles to east-south-east, felspathic sandstones, shales, 
 and black quartzose lydian-stone dip to N. at 40°. The sandstones and shales contain 
 plant-remains. Where the Ravenswood Road crosses the Sellbeim River, about three 
 miles short of the Silver-Mines, there are some coarse conglomerates with a green 
 matrix, and boulders of quartz and quartzite, as well as some green felspathic and 
 quartzose sandstones, all dipping N.N.W. at 45°.+ 
 
 In 1890 Mr. W. H. Rands made a traverse of this district, and reported as 
 follows :— 
 
 “Six miles south of the range dividing St. Paul’s Creek from Cattle Creek, after 
 passing over a reddish sandy soil, flat beds of a fine-grained felspathic sandstone are seen 
 in Cattle Creek, dipping E. 10° N. at 20°. Portions of the sandstone contain a large 
 amount of iron in their composition, and weather red. Above this is a coarse sandstone 
 or grit with the same dip. 
 
 “T found no fossils in these beds, but they are probably Star Beds (Lower Car- 
 boniferous) as they have the same strike and dip as beds of that age met with at Harvest 
 Home and Mount McConnell Stations. 
 
 ‘Continuing southwards towards Harvest Home Station, sandy flats are crossed 
 to within about a mile of the station, where a sandstone dips east-north-east. At 
 Harvest Home, beds of sandstone, with thin beds of shale, dip H.N.E. at 25°. In these 
 I discovered some not very distinct plant-markings (Calamites 7). 
 
 
 
 * See ‘* Catalogue of the Queensland Court in the Colonial and Indian Exhibition” (London Edition), 
 p. 154, 
 
 + See Geological Map attached to Report by R.L.J. on the Sellheim Silver Mines, &c. Brisbane : 
 by Authority : 1889, 
 
136 
 
 “On the south side of the Cape River, opposite to Harvest Home Station, a high 
 ridge occurs coming down close to the river. On the northern flanks of this ridge are 
 similar sandstones dipping steeply east-north-east against a felsitic rock, much resembling 
 that of Mount St. Paul. The ridge is composed chiefly of this rock. 
 
 “The country is quite flat from here across the valley of the Suttor River. 
 
 “ Along the road from Harvest Home Station to Lornesleigh Station, numerous 
 outcrops of sandstones, sandy shales, and quartzites occur, having a general dip towards 
 E. at from 22° to 30°. I could find no fossil remains inthem. A large reef of ‘buck’ 
 quartz crosses the road in a north-north-easterly direction about two miles east of the 
 station. 
 
 “After crossing the Cape River at its junction with the Suttor River, near 
 Lornesleigh Station, the road passes over alluvial flats for a distance of four miles. At 
 this point beds of felspathic sandstone and sandy shales dip H. 35° S. at 20°. These 
 beds are full of stems of Lepidodendron, Calamites, and Cyclostigma ?—a stem with 
 circular leaf-scars. I also found the nearly perfect remains of a fish, which Mr. R. 
 Etheridge, Junr., says certainly belongs to the family Palgoniscide, and probably is of 
 the genus Paleoniscus itself.* 
 
 “The ridges all about here consist of similar beds. About half-a-mile south of 
 this spot there is a bed full of some small, somewhat tripartite nodules which I thought 
 might be Zrigonocarpon, but Mr. Etheridge pronounced them too badly preserved to 
 determine. 
 
 “Between this and Mount McConnell Station, Lepidodendron occurs in many 
 places in the rock. At that station the beds dip south-east. 
 
 “Along the road from Mount McConnell Station to Mount Wyatt, blacksoil 
 flats are traversed for about two miles, and then there is a small boss of granite about 
 two miles across; beyond this the Star Beds occur again, dipping to the north-west for 
 five miles in a south-east direction, and then Gympie Beds come in.t 
 
 “¢ Lepidodendron also occurs in the ridges about two miles east of the station, on 
 the eastern side of the Sellheim River. 
 
 “ Between Mount McConnell Station and Mount McConnell itself, which 
 is about ten miles to the north, the beds are dipping S.E. at 40°. What are 
 known as the ‘Crags’ are on the western side of the road, about seven miles from 
 the station. They are cliffs of hardened sandstone or quartzite of from 50 to 100 feet 
 in height. 
 
 “The rocks immediately south of Mount McConnell consist of beds of sand- 
 stones, fissile shales, and conglomerates, dipping to the south-east at a high angle. The 
 pebbles of the conglomerates consist chiefly of quartz, sandstone, and quartzite. About 
 half-a-mile west of the mountain a thin bed of blue impure limestone dips S.E. 
 at 45°. West of the limestone again, as far as the Suttor River, thin laminated 
 shales occur dipping S.E. at 35°. These shales are full of segregated nodules, of 
 from an inch to nearly a foot in diameter. I searched carefully for any fossil 
 remains about here, butl was only successful in finding a few which were very 
 indistinct. 
 
 “ Mount McConnell itself is composed of felsite. The Star Beds occur as far as 
 the Burdekin, and can be traced six miles or so down the river.” t 
 
 
 
 * The specimen was forwarded to Mr. A. S. Woodward, of the Museum of Natural History, London, 
 who confirmed the reference to Palwoniscus, allowing for the absence of the head. 
 
 + Report on the Sellheim Silver Mines and surrounding District, by R. L. Jack. Brisbane: by 
 Authority : 1889, 
 
 + Report on the Cape River Gold Field, by William H, Rands. Brisbane: by Authority: 1891, p. 16. 
 

 
 137 
 
 At Mount Wyatt, near the head of the Sellheim River, the late Mr. R. Daintree 
 observed “ slightly inclined grits and sandstones of the Upper Devonian Lepidodendron 
 Beds, resting on the upturned edges of a series of blue and grey slates and shales,” 
 which have yielded fossils determined by Prof. McCoy, and referred by him to the 
 Upper Silurian.* The fossils from the “slightly inclined grits and sandstones of the 
 Upper Devonian Lepidodendron Beds,” as determined by Mr. W. Carruthers, F.R.S., 
 and revised by my Colleague, from this locality, are Lepidodendron australe, McCoy, 
 and Cyclostigia, sp. ind. 
 
 From Canoona, near Rockhampton, Mr. Daintree also obtained Lepido-— 
 dendron australe, McCoy, and Cyelostigma, sp., Feist., allied to OC. Kiltorkense.t 
 The former may, as has already been seen, belong to the Rockhampton (Gympie) 
 Beds. 
 
 Mr. Daintree also referst to the Broken River as one of the localities from 
 which he obtained Lepidodendron australe, McCoy. It may be surmised the Lepidoden- 
 dron Beds occur in a horizon equivalent to that of the Star Beds, and separable from 
 the strata which have yielded the Corals described by Prof. H. A. Nicholson and my 
 Colleague (Burdekin Beds). 
 
 In the valley of Machine Creek, on the eastern side of the quartzites and shales 
 (of undetermined age) which, together with intrusive diorites, form the country-rock of 
 the auriferous reefs of Commissioner’s Hill, a considerable thickness of conglomerates 
 and grits and greenish-grey and purple sandstones and shales are met with, the sand- 
 stones containing Lepidodendron australe, McCoy. These beds are seen in two places 
 —the first south of the Gilberton Township, and the second at the head of Star Gully— 
 to overlie the quartzites and shales unconformably, but are faulted against them 
 elsewhere, so far as the boundary has been traced. There can be little doubt that these 
 beds belong to the Star Formation. 
 
 From the Northern area, which may be considered as the type district of the 
 Star Formation (including Star, Keelbottom, Harvest Home, and Mount Wyatt), the 
 following fossils have been derived, as per my Colleague’s revised list :— 
 
 Lepidodendron australe, McCoy. 
 
 rs sp. ind., Pl. 6, figs. 1, 4. 
 
 Cyclostigma, sp., Feist., allied to C. Kiltorkense. 
 
 Actinocrinus, sp. ind., Pl. 7, fig. 9 
 
 Beyrichia varicosa, T. R. ape Pl, 7, fig. 15. 
 
 Phillipsia dubia, Eth., Pl. 7, fig. 12; Pl. 8, figs. 5,6; Pl. 44, fig. 4. 
 
 Fenestella multiporata, De Kon., Pl. 8, figs. 7, 8. 
 
 Spirifera bicarinata, Hih. fil., Pl. 10, figs. 9,13; Pl. 37, fig. 17; Pl. 11, 
 figs. 1-3. 
 
 Spiriferina duodecemcostata, McCoy, Pl. 44, fig. 12. 
 
 Reticularia Urei, Fleming. 
 
 Retzia radialis, Phill., Pl. 11, figs. 24, 25. 
 
 Rhynchonella pleurodon, Phill., Pl. 11, fig. 23. 
 
 Orthis resupinata, Martin, P]. 11, figs. 26, 28. 
 
 Strophomena rhomboidalis, var. analoga, Phill., Pl. 12, figs. 8, 9; Pl. 40, 
 fig. 6. 
 
 Chonetes cracowensis, Eth., Pl. 13, fig. 9 
 
 
 
 
 
 * Daintree, General Report upon the Northern District. Brisbane: by Authority : 1870, p. 7. 
 + Quart. Journ. Geol. Soc. (1872), xxviii., p. 289. 
 + Loc. cit. 
 
138 
 
 Chonetes, sp. ind. (a), Pl. 18, fig. 10; Pl. 87, figs. 21, 22. 
 “ spetnd, (ce), Pl. 37, tig. 20. 
 
 Entolium, sp. 
 
 Huchondria, sp. 
 
 Nucula, sp. ind., Pl. 40, fig. 10. 
 
 Nuculana, sp. ind., Pl. 14, fig, 17. 
 
 Naticopsis variata, Phill. ? 
 es sp. ind. 
 
 Porcellia Pearsi, Eth. fil., Pl. 15, figs. 7, 8. 
 
 Orthoceras, sp. 
 
 Paleoniscid Fish. 
 
 From the Drummond Range a number of fossils have been obtained by the late 
 Rev. J. E. Tenison Woods, Mr. W. Fryar, Mr. A. E. Holmes, Mr. C. T. Musson, and 
 the late Mr. James Smith, which enable us to place the strata in which they occur on 
 the horizon of the Star Beds. The strata of the Drummond Range, of which the 
 cuttings on the Central Railway afford admirable sections, do not bear any strong 
 resemblance to the Star Beds of the Northern areas. ‘Three miles and a-half east of 
 Pine Hill Station (248}-mile peg) yellow gritty sandstones and shales are seen dipping 
 at 7° to W.—a dip which would carry them beneath the Desert Sandstone. At 
 243 miles similar sandstones dip to S. at 12°. From Hannam’s Gap (2385 miles) 
 to Bogantungan (227 miles) the strata consist of finely laminated, fine-grained, blue- 
 grey sandstone, and blue, grey, and greenish, and occasionally purple, shales. Thick 
 beds of hard gritty white, yellow, or brown siliceous sandstone occur at intervals. From 
 Hannam’s Gap to Bogantungan the strata dip at an average angle of about 2° to E. 
 (a little steeper than the grade of the railway). At Bogantungan is the axis of a 
 synclinal trough, and as far eastward as Withersfield the dip is towards the west. The 
 total thickness of the strata is probably not less than 2,000 feet. According to the 
 railway survey Pine Hill Station is 1,158 feet; Drummond (241 miles), 1,450 feet ; 
 Hannam’s Gap, 1,717 feet; Bogantungan, 1,098 feet; and Withersfield, 834 feet above 
 the sea-level. 
 
 Early in 1890 (?) Mr. C. T. Musson, F.L.S., presented to the Mining and 
 Geological Museum, Sydney, numerous pieces of greenish-grey sandy micaceous shale, 
 with small fish scales and plates scattered over them, from a locality in the Drummond 
 Range which he described as follows :— 
 
 “On and around a small ridge, half-a-mile from and to the north of the Bogan- 
 tungan Railway Station, I found numerous fish-remains consisting of scales and spines 
 in nodules from what appear to be Carboniferous shales, the beds dipping east, and 
 apparentiy continuous with those of a similar character developed at the east end of the 
 cutting in the range, some two or three miles away. The fossils occur in nodules, 
 which are seen to rest in thin bands in a section showing hard and soft beds of a 
 peculiar dark-greenish clay (mapped Carboniferous by the Geological Survey), with 
 other harder bands in thin layers, which are sometimes seen to cap the ridges. The 
 fossils were found dn situ, and lying about the gullies, of which there are three. The 
 beds rest on a coarse gritty rock in places of a crystalline character. The hard 
 fossiliferous bands vary considerably in themselves, and show evidence of having been 
 altered from their original condition.” * 
 
 * “ Note on the Occurrence of Fish Remains in the Rocks of the Drummond Range, Central Queens- 
 land.” By R, Etheridge, Junr. Records Geol. Survey New South Wales, Vol. ti., Pt. 2, 1890, p. 72. 
 

 
 NE 
 
 139 
 
 Of these remains Mr. Etheridge says *: “On examining the scales and other 
 plates they struck me at once as those of a Palzoniscid, but before finally adopting 
 this view I forwarded drawings to Mr. A. 8. Woodward, of the British Museum, who 
 confirmed it.” 
 
 Mr. James Smith, having been sent to collect from this locality, made a report 
 dated 23rd March, 1891—the last received from him—which, though tinged with the 
 pardonable exaltation of an enthusiastic naturalist, is as full of shrewd observation as 
 any of his earlier writings, and may be quoted in full as practically his “last words” 
 to the scientific world. On 4th April Mr. Smith returned to Rockhampton from a 
 collecting trip to Springsure, suffering from the effects of exposure and repeated 
 wettings, and on 10th April expired. 
 
 “The mud shales [of the Drummond Range] are very susceptible to decomposi- 
 tion. The action of the atmosphere crumbles them rapidly back into the dust from 
 which they came. They are eaten out from between the sandstone beds, which, left 
 without support, topple down and encumber the slopes of the hills, showing to 
 advantage the process of denudation. Or they stretch along for miles in over- 
 hanging cliffs, giving variety to the view. By this process glens and gorges a thousand 
 feet deep have been excavated, forming the magnificent landscapes of the Drummond 
 Range. 
 
 “The numerous railway cuttings, some of them forty feet deep, afford splendid 
 sections for studying the character of the formation. I made sixty traverses, on foot 
 and by rail, of these cuttings, and adjacent creeks and gullies; examined all the spill- 
 banks and rock-shelyes. After the most careful observations I could see no sign of 
 any organism, in any of the shales. 
 
 * “Tt is in and on the sandstones the harvests of the collector's treasures can be 
 gathered—an abundant land flora, a still more abundant marine fauna. 
 
 “The plant-remains are Cyclostigma, Lepidodendron, and Calamites of various 
 kinds, beautifully marked, fluted, and grooved. These have been determined in the 
 Rey. Mr. Tenison Woods’ work on the ‘ Fossil Flora of the Coal Deposits of Australia,’ 
 and they are in great abundance. In every spill-bank, in every creek, they are printed 
 on and in the rocks, in promiscuous confusion, as if wafted to a shore and sanded up, or 
 water-logged and sinking to the bottom. 
 
 “Then there is the great fish-bed. A band of fine-grained, finely stratified, grey 
 sandstone, twelve inches thick—the lowest band of the cutting at Hannam’s Gap. 
 This band has been excavated, and cast aside on spill-banks, on both sides of the 
 railway. The centre of the band is black, and has the appearance of anthracite, 
 derived, I believe, from the matter of the fishes’ bodies. The scales in this centre part 
 are very black and glistening, the bones merely black films. The action of the air has 
 left this middle part all gaping open in parallel fissures. It is on both sides of this 
 centre band, throughout the rest of the body of the stone, that the fish-remains are 
 in better preservation. They consist of bones, scales, spines, and fins, in marvellous 
 abundance. Among the fins are heterocercal fish-tails. There are also oolitic struc- 
 tures, which I suggest may be the spawn of fishes. Although there are some curved 
 bones, like retractile teeth, two inches long and half-an-inch thick at the base, yet 
 upon the whole I think the fishes were of small size; the fins are only a little longer 
 than those of a haddock. The rhomboid scales, with comma-like attachment, are 
 beautifully wrinkled. The triangular ones are deeply serrated on the sides and 
 wrinkled on the back, while the ‘ oat-shaped’ (th. Junr.) ones have a short groove in 
 
 
 
 PLCs Cite 
 
140 
 
 the back, for the overlapping point of the next one to liein. Do these three different 
 sets of scales indicate different fishes of the same family ? 
 
 “ One thing the specimens will prove. They must have been in most incredible 
 numbers, like a herring shoal, in length, breadth, and thickness. Outcrops of the 
 known bed are found nine miles apart. The width has not yet been ascertained. 
 
 “My instructions were to look out for and collect fish-remains. Unfortunately 
 you cannot bag a spill-bank, nor can a railway train carry it away. It will be a long 
 day hence before all the oe -remains of the Drummond Range are in museums. I 
 brought away eight bushels. 
 
 “‘T did not see any of the crystalline rocks im situ mentioned by Mr. Musson, 
 although there are plenty of water-worn crystalline boulders, in the alluvium of 
 the Bogantungan Creek banks. I prefer to believe these are from some dyke in 
 the upper ranges, for on going two miles lower down the creek, at a much lower 
 level, the indurated stratified ferruginous lower sandstone bed still rests on stratified 
 shales. It was here I found the largest Calamite zm stu, and they are found in 
 all the sandstone beds up to the summit, showing a long period of growing some- 
 where, and then being carried to the point of deposition in the sandstone-forming 
 beds. 
 
 “There is a thin band of limy marl runs along for miles, near the bottom of all 
 the cuttings. There are numerous hand-size crystallised septaria concretions, of which 
 I secured specimens. At the 237-mile the sandstones are splendid slabs, four to five 
 feet square, enough to pave a city—hard and indurated, recalling memories of the 
 Arbroath slabs (Lyell’s Elements, p. 403).” 
 
 These fish-remains form an additional and strong link connecting the Drummond 
 and Star Beds. Mr. Smith’s fossils have not yet been examined. 
 
 My Colleague’s revised List of Fossils from the Drummond Range is as follows:— 
 
 Calamites varians, Germar. 
 Asterocalamites scrobriculatus, Schloth. 
 Aneimites austrina, Eth. fil. 
 Lepidodendron australe, McCoy. 
 be veltheimianum, Sternb. 
 sp. ind., Pl. 6, figs. 1, 4. 
 Cet ie australe, Read p 
 Stigmaria, sp. ind., Ten. Woods. 
 Cordaites australis, McCoy ? 
 Palzeoniscid Fish Remains. 
 
 It will be seen that, up to the present time, the Drummond Beds have yielded a 
 longer list of plants than the Star, while on the other hand the Star Beds have a 
 considerable number of marine organisms which are not represented, so far as we 
 know, in the Drummond Range, with the exception of Paloniscid fish, which are 
 common to both. 
 
 At Elgin Downs, sixty-five miles east of Clermont, Mr. Rogers-Harrison obtained 
 Lepidodendron, Calamites (?), and what was “ probably the fruit of a conifer.” * There 
 is no information available with regard to the strata from which these plant-remains 
 came, but it is not improbable that they are the equivalents of the Star or Drum- 
 mond Beds. 
 
 Grouping the whole of the above localities together, including the Star proper, 
 Keelbottom, Harvest Home, Mount Wyatt, Canoona, Broken River, and the Drummond 
 
 
 
 * Report on the Geology, &c., of the Country in the Vicinity of Clermont. By W. H. Rands. 
 Brisbane: by Authority : 1886, p. 3. 
 
Range, under the head of the ‘Star Beds,” the complete list of fossils, as revised by 
 
 my Colleague, is as follows :— 
 
 Calamites varians, Germar. 
 Asterocalamites scrobriculatus, Schloth. 
 Aneimites austrina, Eth. fil. 
 Lepidodendron australe, McCoy. 
 
 . veltheimianum, Sternb. 
 
 " sp. ind., Pl. 6, figs. 1, 4. 
 Cyclostigma australe, Feist. ? 
 
 - sp., Feist., allied to C. Kil- 
 torkense. 
 
 Stigmaria, sp. ind., Ten. Woods. 
 Cordaites australis, McCoy. 
 Actinocrinus, sp. ind., Pl. 7, f. 9. 
 Beyrichia varicosa, T. R. Jones. 
 Phillipsia dubia, Eth. 
 Fenestella multiporata, De Kon. 
 Spirifera bicarinata, Eth. fil. 
 Spiriferina, sp. ind, 
 
 
 
 Reticularia Urei, Fleming. 
 Retzia radialis, Phill. 
 Rhynchonella pleurodon, Phill. 
 Orthis resupinata, Martin. 
 Strophomena rhomboidalis, var. analoga, 
 Phill. 
 Chonetes cracowensis, Eth. 
 ss sp. ind. (a), Pl, 13, f. 10. 
 5 sp. ind. (c), Pl. 37, £. 20. 
 Entolium, sp. 
 Euchondria, sp. 
 Nuculana, sp. ind., Pl. 14, f. 17. 
 Naticopsis variata, Phill. ? 
 5 sp. tnd. 
 Porcellia Pearsi, Eth. fil. 
 Orthoceras, sp. 
 Paleoniscid Fish. 
 
 
 
 Of the above fossils, Lepidodendron australe, Cordaites australis, Actinocrinus, sp. 
 ind., Phillipsia dubia, Spirifera bicarinata, Rhynchonella pleurodon, Orthis resupinata, 
 and Strophomena rhomboidalis, var. analoga, are common to the Star and Gympie 
 Formations ; Chonetes cracowensis, Porcellia Pearsi, and Orthoceras are common to the 
 Star and Gympie Formations and the Middle Series of the Bowen River Coal Field; the 
 remainder, viz., Calamites varians, Asterocalamites scrobriculatus, Aneimites austrina, 
 Lepidodendron veltheimianum, L. sp. ind. (Pl. 6, figs. 1, 4), Cyclostigma australe ? C. sp. 
 all. to C. Kiltorkense, Stigmaria, sp. ind., Beyrichia varicosa, Fenestella multiporata, 
 Spiriferina, sp.ind., Reticularia Urei, Retzia radialis, Chonetes, sp. ind. (a), Chonetes, sp. 
 ind. (¢), Entolium, sp., Euchondria, sp., Nuculana, sp. ind., Naticopsis variata, Naticopsis, 
 sp. ind., and the Paleoniscid Fish, are peculiar to the Star Beds. 
 
 The Star Beds have not a single species, so far as we yet know, common to the 
 (Middle Devonian) Burdekin Beds. 
 
 Comparing the genera represented in the Star Beds with those of the other 
 members of the Permo-Carboniferous System, we find that, among Plants, Calamites, 
 Lepidodendron, and Cordaites are also present in the Gympie Formation. Among 
 Crinoids, Actinocrinus, and among Crustaceans, Phillipsia, are common to both. Among 
 Polyzoa, Fenestella is present in both. Lastly, the two formations have nine genera of 
 Mollusca in common—viz., Spirifera, Reticularia, Retzia, Rhynchonella, Orthis, Stropho- 
 mena, Chonetes, Naticopsis, and Porcellia. 
 
 Common to the Star and Middle Bowen Formations are one genus of Polyzoa, 
 viz., Fenestella, and five of Mollusca, viz., Spirifera, Spiriferina, Chonetes, Porcellia, 
 and Orthoceras. 
 
 There are not even any genera common to the Star and Upper Bowen For- 
 mations. 
 
 The late Mr. C. 8S. Wilkinson, Government Geologist for New South Wales, in 
 “Mines and Mineral Statistics of New South Wales, 1875,’* observed that ‘‘ Below 
 the lower marine beds of the Hunter district are beds of shales and sandstones, 
 
 * Page 132. 
 
142 
 
 with several species of Cyclopteris, Knorria, Sigillaria, Stigmaria, Lepidodendron, &c. 
 
 aon They occur near to, and probably in association with, beds of marine 
 Hele which have been described’ as lower carboniferous.” These fede which are 
 particularly well developed in the neighbourhood of Stroud, I believe to be on the same 
 horizon as the Star Formation; but no passage has ever been observed in New South 
 Wales from the Lepidodendron Beds referred to, upwards into the marine beds of the 
 Hunter district. 
 
 In his “ Notes on the Geology of New South Wales,”* Mr. Wilkinson says :— 
 “Near Canowindra, on the Lachlan River, are ranges composed of purple and white 
 sandstones and shales containing Lepidodendron and Sigillaria. The Weddin Moun- 
 tains and those conspicuous hills beyond Condobolin consist of similar rocks, which may 
 also belong to this age, or to the Upper Devonian, but as yet no fossils have been found 
 in them. The lower beds are extensively developed between the Hunter and the 
 Manning Rivers, where they form high broken ranges. They consist of conglomerates, 
 sandstones, Hmestones, and shales, which have been much disturbed, being tilted at 
 all angles. Near Gloucester there is a splendid natural section showing, ee a distance 
 of more than a mile, the beds in a vertical position. Though plant-remains are 
 abundant in these rocks, no workable coal-seams are known. This is somewhat 
 remarkable, seeing that the fossils are of the genera which are characteristic of the 
 great Coal Measures of England—viz., Lepidodendron, Sigillaria, and Calamites. The 
 gold-bearing quartz reefs yielding from 1 to 15 oz. of gold per ton, now being worked 
 on the Copeland Gold Field, traverse strata containing these fossils.+ There are other 
 beds in the same series rich in marine fossils—Productus, Spirifer, Crinotds, Fenes- 
 tella, &e.” 
 
 It is possible that the Avon River Lepidodendron Beds, Victoria, may be 
 approximately on the horizon of the Star Formation. 
 
 J. 
 
 ss ee ee ee 
 * Sydney : Government Printer: 1882. 
 
 + So far as the fossils show, these beds may be equivalent to our Gympie Beds, 
 
CHAPTER XI. 
 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 THE BOWEN RIVER COAL FIELD 
 AND Its SUBDIVISIONS, 
 
 Tue Coalfield, which extends from the Bowen River in Lat. 20° 30' southward to the 
 heads of the Dawson in Lat. 26°, is capable of subdivision into three distinct formations: 
 a Lower, in which no organic remains have as yet been discovered, and which is, in the 
 Mackay District, considerably altered, and in the Bowen River is divided from the 
 succeeding formation by a series of bedded volcanic rocks; a Middle, rich in organic 
 remains, chiefly of marine origin, but with an admixture of the remains of a terrestrial 
 vegetation ; and finally an Upper, full of the remains of a land vegetation (of which 
 one genus at least, viz., Glossopteris, is common to the Middle Formation), but with at 
 least one intercalated bed in which characteristic species of the marine fauna of the 
 Middle Formation reappear. The three formations form a continuous series. 
 
 Following Daintree, I divided, in my Geological Map of the Colony issued in 
 1886, the Bowen River Coal Field from the Coal Field of the Isaacs, Mackenzie, and 
 Dawson lying to the south; Daintree’s Map, issued in 1872, showing an extension of 
 the basaltic area of Peak Downs, to the north-west and north of the latter field. Since 
 then, however, Mr. Maitland has examined the intervening district,* and shown that 
 the Bowen and Mackenzie Coal Fields are in reality continuous, although covered, at the 
 heads of the Bowen, Suttor, and Isaacs Rivers, by outlying tablelands of the Desert 
 Sandstone. 
 
 In my Geological Map (1886), the whole of the Mackenzie Coal Field was ascribed 
 to the Upper Formation, as it had never been examined in detail. The Geological Map 
 issued herewith, however, shows that the Upper Formation is flanked to east and west 
 by members of the Middle Formation—an alteration which is justified by Mr. Maitland’s 
 and my own work in the field in the neighbourhood of Nebo, by Mr. Rands’ observations 
 in the Clermont District, by Mr. Smith’s discoveries of characteristic “ Middle” fossils 
 at Springsure and Banana Creek, and by Mr. Daintree’s recorded observations at 
 Cracow Creek, In the southern portion of this district, however, no detailed mapping 
 has ever been done, and the dividing line between the Middle and Upper Formations 
 has not been traced, and consequently cannot be supposed to have been laid down 
 accurately on the map. 
 
 In the year 1878 I made a detailed survey of the Bowen River Coal Field,t 
 separating, for the first time, the Lower, Middle, and Upper Formations. A description 
 of these subdivisions is given in the succeeding chapters. 
 
 J. 
 
 
 
 * Report on Geological Observations at the Heads of the Isaacs, the Suttor, and the Bowen Rivers 
 Brisbane: by Authority: 1889; and Annual Progress Report of the Geological Survey for 1889 
 Brisbane : by Authority : 1890. 
 
 + Report on the Bowen River Coal Field, Brisbane: by Authority: 1879, 
 
CHAPTER XII. 
 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 THE LOWER BOWEN FORMATION IN THE TYPE DISTRICT. 
 
 In the district from which this series receives its name, and in which it was first 
 mapped, the granite, schists, slates, and other plutonic and metamorphic rocks of the 
 Clarke Range are succeeded by a thick accumulation of coarse volcanic agglomerate, 
 made up of angular or but little rounded pebbles and boulders. On this agglomerate 
 lie thick beds of conglomerate, the pebbles of which are mainly of quartzite and yellow 
 porphyry derived from the surrounding metamorphic country, but afew are of porphyrite, 
 &¢c., derived from the immediately underlying bed of volcanic agglomerate. To the con- 
 glomerate succeeds a mass of yellow siliceous sandstone, at least fifty feet in thickness 
 and probably much more. Soft stratified rocks of a similar character evidently crop 
 out all over the plain which extends southward from a little mountain about three miles 
 below the head of Pelican Creek to Mount Devlin, under whose steep escarpment they 
 dip and disappear. As the breadth of this flat is about a mile, a dip of 10° would give 
 a thickness of about eight hundred and eighty feet. 
 
 The Bowen and Sonoma Road, between Bolger’s (ruined) Public-house and Strath- 
 more Creek, crosses the outcrops of several beds of white and yellow sandstones, dipping 
 at a low angle to the south-east. This dip would carry the sandstones beneath the 
 porphyrites, which are first met with near Strathmore Creek, and which presently rise 
 in terraces in the Mount Toussaint Range. From their position, resting on the meta- 
 morphie rocks and underlying the bedded traps, there can be no doubt that the 
 sandstone beds in question are the equivalents of those which, at the head of Pelican 
 Creek, dip under the traps of Mount Devlin. 
 
 INTERBEDDED PORPHYRITES AND BASALTS. 
 
 The voleaniec range of Mount Toussaint and Mount Devlin presents the usual 
 features characteristic of slightly inclined trappean rocks. The range appears very 
 different according as it is viewed from the “dip” or “rise” side of the beds. In the 
 one case the long gentle slope of the hill generally coincides with the surface of a bed. 
 In the other the ascent must be made over a series of alternate terraces and almost 
 perpendicular cliffs. 
 
 Over considerable areas basalts and melaphyres decompose to a rich black soil. 
 The amygdaloidal porphyrites form a lighter but still very good soil. 
 
 The terraced and scarped hills of the Mount Macedon Range continue the 
 outcrop of the bedded trap round the north-western corner of the coalfield. 
 
 It is difficult to find, either in the Mount Macedon or Toussaint Range, a hand 
 specimen of the trappean rock which has not obviously undergone considerable 
 alteration. A specimen from the south end of Mount Macedon, which appeared more 
 than usually fresh, was sliced and examined microscopically. The ground-mass showed 
 a tangled web of very minute interlacing crystals of labradorite, the interstices filled 
 up with specks of magnetic iron. The augite crystals were generally represented by a 
 zeolitic pseudomorph (prehnite?), although occasionally a nucleus of augite could be 
 
145 
 
 detected in the centre of an altered mass. The rock was thus, in all likelihood, 
 originally a typical dolerite. It is not surprising that igneous rocks so ancient should 
 have undergone much alteration. 
 
 On Strathmore Creek, on Pelican Creek from Mount Bellavista downwards, and 
 in the Bowen River at the north end of the coalfield, the rock is exceedingly amygdal- 
 oidal, and is full of cavities, sometimes of considerable size, filled up with prehnite, 
 thomsonite, analcime, or laumonite. With the prehnite, carbonate of copper is frequently 
 associated, some specimens of the ore being quite good enough to work if sufficient 
 quantities could be obtained. The ore, however, so far as I was able to see or learn, 
 nowhere occurs in lodes. 
 
 Mr. Samuel Allport, F.G.S., thus reports* on the microscopic aspect of 
 ““Hpidote rock’’ from the “ Bowen River, near McDougal’s head station” (Birallee, 
 now Mr. Hughes’s) :— 
 
 ‘Tt must have been originally as scoriaceous as any recent lavas, but now forms 
 a hard solid mass of zeolitic mineral matter. All the cavities are filled with prehnite 
 in radiating groups of crystals, which exhibit a magnificent display of colours when 
 examined in polarised light. One cavity is lined with the radiating prehnite, and the 
 central portion partly filled with calcite and partly with carbonate of copper. Of the 
 original constituents nothing is left except the magnetite. The forms of felspar 
 crystals are sharp and distinct; but the original substance has been removed and 
 replaced by prehnite, differing in no respect from that filling the cavities. The reddish- 
 brown grains and patches scattered through the base probably represent the augite.” 
 
 In the Mount Toussaint and Mount Macedon Ranges, as well as in the bed of 
 the Bowen River and Pelican Creek, geodes of opal, agate, and chalcedony are not 
 unfrequently met with. 
 
 J. 
 
 * Quart, Journ, Geol, Soc., xxxviii., p. 315, 
 
CHAPTER XIII. 
 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 THE LOWER BOWEN FORMATION OUTSIDE OF THE TYPE DISTRICT—MACKAY 
 DISTRICT. 
 
 Tue interbedded basalts, &c., between the Middle and Lower Series are not seen along 
 the junction line south of the heads of the Bowen River, so that it appears that a fault, 
 which further north throws the basalts, &c., against the metamorphic rocks, to the south 
 throws the Middle down against the Lower Series. 
 
 The Lower Formation in the coast region, although possessing many of the 
 characteristics of the same series in the district north of the Bowen River Coal Field, is 
 much better developed and occupies a much larger extent of country. Owing to the 
 intrusion of voleanic rocks no trustworthy estimate of its thickness can be made, but 
 making allowance for all contingencies the thickness is probably not less than 1,000 feet. 
 
 At Mount De Moleyn on the north bank of the Pioneer River, west of Mackay, 
 the Lower Series rests upon a coarse volcanic agglomerate resembling that which occurs 
 at the head of Pelican Creek. South of the Pioneer River, the Lower Series attains a 
 ereat thickness, and has been penetrated by granites, dolerites, and basalts, which in 
 many cases alter the strata in contact with them for a considerable distance. At the 
 heads of the Pioneer a gradual passage from a comparatively unaltered sandstone into a 
 granite can be observed ; in no case, however, has the metamorphism gone so far as to 
 entirely mask the clastic character of the rock. 
 
 “Tt is a noteworthy circumstance that it is in this, the lowest member of the 
 series, that the greatest amount of metamorphism has taken place. Indeed no section was 
 seen in which it could be confidently asserted that the granitic rocks penetrate the 
 higher members of the series.” Mr. Maitland observes that this circumstance may 
 indicate that a sufficient time elapsed to allow of the metamorphism of portions of the 
 Lower Series before the Middle Series was deposited. 
 
 In the area drained by Rocky Dam Creek, south-west of Mount Funnel, ie rocks 
 of the Lower Series have undergone much alteration, some of the grits assuming the 
 appearance of quartz-felsites, whilst some sandstones have been altered into quartzites 
 North of Mount Funnel horizontal beds of conglomerate and sandstone, of various 
 degrees of colour and texture, are exposed in several gullies; near Mount Selwyn one 
 bed is a green felspathic conglomerate, in which clear and pellucid blebs of quartz 
 appear to have been developed subsequent to its deposition. 
 
 Where the St. Lawrence Road crosses Rocky Dam Creek a bed of coarse grit is 
 seen, dipping at a low angle to the east. JF urther up the creek, on its southern bank, 
 in Selection 1442, is a low hill of dolerite, probably intrusive through the sedimentary 
 rocks. In the bed of the creek, higher up, an altered sandstone is seen, and on a 
 mountain bearing 52° 50’ from Mount Funnel, the seaward face consists of a great 
 thickness of an altered conglomerate, penetrated by a dyke of felsite. 
 
 A spur on the western face of Cone Mountain is made up of a massive quartzite, 
 apparently horizontal From this point, in a traverse northward across Rocky Dam 
 and Arrowroot Creeks to the Eildon Hills, altered sandstone and shales are seen at 
 intervals. 
 
147 
 
 On one of the branches of Cherry-tree Creek, flowing through Selection 1531, 
 a baked black shale is seen dipping E.S.E. at 35°, and what appears to be a volcanic 
 breccia is visible close to the great mass of rock mapped as diorite, which occupies a 
 considerable area of country close to the St. Lawrence Road. 
 
 In the bed of Cherry-tree Creek, about three-quarters of a mile north-east of 
 the house in Selection 1569, a mass of felsite has been protruded through reddish-brown 
 shales and conglomerates, spreading out over the surface of the conglomerate. Both 
 the conglomerate and the underlying shales have been altered by the felsite. Higher 
 up the creek is a great thickness of conglomerate, very coarse-grained at the base but 
 finer above. In the upper portion of the conglomerate, much felspar, a little quartz, 
 and some iron pyrites have been developed in the mass. A dyke of felsite intersects 
 the conglomerate. Near the head of the creek an intrusive mass of granite forms the 
 summit of the range. 
 
 Between Cherry-tree and Plum-tree Creeks the prevailing rocks consist of altered 
 grits, conglomerates, and sandstones, in horizontal beds. A felsite dyke intersects the 
 stratified rocks, in which, near the dyke, secondary crystals and crystalline grains of 
 quartz are developed. 
 
 In Alligator Creek, one of the heads of Atherton’s Creek, a mass of sedimentary 
 rocks, with a contemporaneous sheet of diorite, are pierced by protrusions of felsitic 
 rocks, as sketched in Plate 53, fig. 1. From the base of the felstone sheet to the top of 
 the grit forming the summit of the range is two hundred and sixty feet. 
 
 In Bell’s Creek, a branch of Atherton’s Creek, the section sketched in Plate 53, 
 fig. 2, is seen. Ona thick series of grits and shales which dip W.S.W. at from 15° to 
 20°, lies an intrusive (?) sheet of a porphyritic felsite. Above the felsite are greyish- 
 yellow shales and sandstones, one bed of shale being crowded with imperfectly preserved 
 plant-remains. An intrusive boss of diorite is erupted through the sedimentary rocks 
 and felsite, altering the shales into lydian-stone and the grits into quartzite. Above the 
 greyish-yellow shale and sandstone are dark shales and grits, dipping to S8.8S.W. at 10°. 
 Through these rocks a sheet of felsite has been intruded along the planes of bedding. 
 This sheet is doubtless connected with a vertical dyke of a similar rock seen a little 
 higher up the creek. About 1,000 feet above the lowest beds of the section a mass of 
 felsite, twelve or fourteen feet thick, has been intruded along the bedding planes of 
 the shales and sandstones. Above the felsite are shales and sandstones up to the 
 summit of the range. 
 
 In a gully, a tributary of Sandy Creek, behind Oakenden Plantation, a granitic 
 dyke, somewhat similar in character to the granite of the Mount Bridgman Range, 
 penetrates shales and sandstones, indurating the former and converting the latter into 
 quartzite. 
 
 In a creek parallel to the last and also running into Sandy Creek, shales and 
 altered grits, dipping at 15° to S.W., are accompanied by sheets of basalt, apparently 
 intrusive, the basalt and stratified rocks both penetrated by a granitic dyke. 
 
 Near Homebush Hill, altered shales and sandstones penetrated by a dyke of 
 quartz-felsite occur. Remains of reed-like plants and fragments of silicified wood are 
 common, but too indistinct for determination. In a creek crossing the boundary of 
 Portions 775 and 1603, sandy shales, dipping at 20° to 25° to E.N.E., are interrupted 
 by a sheet of felspar porphyry. At Selection 1880, sandstones and shales are seen in a 
 gully, the former containing fragments of silicified wood and the latter plant-remains. 
 
 One of the branches of Cut Creek shows alternations of sandstones and shales 
 with intrusive diorite; following up the gully until, due east of Mount McBride, a 
 horizontal bed of altered conglomerate is seen. 
 
148 
 
 Pioneer River.—The country drained by the Pioneer River and its tributaries 
 is rudely triangular in shape, and of about six hundred square miles in extent, but by 
 far the greater portion is occupied by crystalline rocks and alluvial soil. It is only here 
 and there that any sedimentary rocks are seen. 
 
 In the bed of the Pioneer, near Dumbleton, is an exposure of intensely 
 metamorphosed sandstones, grits, and shales, with intrusive dykes of basalt and diorite. 
 Higher up the river, below the bridge at Pleystowe Mill, is a series of black shales 
 showing little or no alteration beyond a slight increase in hardness within a couple of 
 inches of a dyke of diorite-porphyrite with which the rocks are associated. 
 
 In the hills to the south of Ashburton Mill, sandstones and shales dip W. at 
 25° to 80°, and a bed of voleanic ash oceurs among the sedimentary rocks. 
 
 In the hills between Ashburton and the Bowen Road, black, slightly indurated 
 shales dip at 15° to E.N.E. Black Waterholes Creek rises in a deep, scrubby gorge, 
 whose sides show sections of coarse altered sandstones and grits, below which black 
 sandy shales are seen to dip to HE. at an angle of 10°. One of the main tributaries 
 of Black Waterholes Creek shows a quartzite underlaid by a very hard lydianised shale 
 lying horizontally. Further up the creek, in Selections 1602 and 1414, the rocks are 
 pierced by an intrusive granite. Lower down the creek, greyish sandstones and black 
 shales dip at 15° to W. 
 
 Several other tributaries of the Pioneer show sandstones and grits, all more or 
 less metamorphosed, so much so in some places that, in the absence of “ bedding-planes,”’ 
 ripple-marks, &c., they might easily be mistaken for some forms of granite. 
 
 On the spurs of the Main Range, between Cattle Creek and a tributary named 
 Dalrymple Creek, the gradual passage from a comparatively unaltered grit into a granite 
 can be satisfactorily traced. Starting with a grit showing distinct traces of bedding, a 
 quartzite is next seen, passing in turn into what appears to be a porphyritic felsite, and 
 ending in a true granite. Several similar instances can be seen in this area. <A 
 noteworthy case occurs near Snake Hill, on the divide between the waters of Black’s 
 Creek and Stockyard Creek. Here a micaceous sandstone merges almost insensibly 
 into a medium-grained granite. 
 
 At several places along the slopes of the hills on the southern banks of the 
 Pioneer, near the Blue Mountains, horizontal sandstones and shales are interstratified 
 with lavas and ashes. 
 
 In the Parish of Bong Bong, opposite Selection 1221, a bed of fine-grained diorite 
 overlies a horizontal bed of grit. Farther up the hill a bed of volcanic ash, composed 
 of subangular fragments of rock, rests on the diorite. 
 
 In the bed of Constant Creek, below Selection 756, a bed of black shale, dipping 
 S.S.W. at 10°, contains three bands of fireclay, varying from one to four inches in 
 thickness. These have often imbedded among them flat circular concretionary siliceous 
 nodules. In Selection 1858 the shales are vertical and are faulted against a fine-grained 
 sandstone. In the Township Reserve, east of Mount Jukes, sandstones and shales, with 
 an intrusive orthoclase porphyry, dip at 20° to N.W. Constant Creek rises in the 
 Mount Toby Range, and flows over alternations of grit and shale, which here roll about 
 a good deal, and are well seen in the Bowen Road, between the Leap and Jolimont 
 Station. 
 
 Murray Creek rises in one of the spurs of Mount Dalrymple, and drains an area 
 mainly composed of crystalline rocks. The only tributary it receives whose waters 
 flow over sedimentary rocks is Jolimont Creek. 
 
 On one of the branches of Jolimont Creek, behind the Beaumont Store, are 
 black shales, with one or two highly carbonaceous bands, semi-vitreous white sandstones, 
 
149 
 and massive fine-grained sandstone slightly indurated. A sheet of intrusive felsite 
 occurs in the black shales and semi-vitreous sandstones. The whole series rests on 
 diorite. In the bed of the creek, below the store, a sheet of diorite is seen overlying 
 a bed of argillaceous shale. 
 
 At the foot of Mount Roy, on the western bank of Jolimont Creek, a white 
 semi-vitreous grit rests on decomposed diorite, and is succeeded by a contemporaneous 
 sheet of dolerite, ten feet in thickness. The dolerite is overlaid by a thick mass of 
 white semi-vitreous sandstone, quartzose, conglomerate, and yellowish grit, the whole. 
 dipping at 5° to 8° N.W. 
 
 An outcrop of semi-vitreous sandstone is seen near Palm-tree Creek, on the 
 Bowen Road. Some portions of this rock appear as if a second deposition of quartz had 
 taken place subsequent to its formation. The sandstone rests on a volcanic ash or fine 
 agglomerate. 
 
 In a quarry further north along the Bowen Road a contemporaneous sheet of 
 diorite, two feet thick, weathering into spheroidal masses, is overlaid by beds of argil- 
 laceous shale which dip to 8.E. at 40° beneath dioritic lava. 
 
 On the south bank of St. Helen’s Creek, and about two miles from the road, the 
 sedimentary rocks lie directly on an uneven surface of felspar porphyry. The escarp- 
 ment of the stratiform rocks can be traced for a considerable distance, and is well seen 
 where the creek cuts its way through a narrow gorge, whose flanks are made up of beds 
 of semi-vitreous sandstone and coarse conglomerate dipping at 5° to W. 
 
 A lew gap ina range between St. Helen’s Head Station and Mount Barren is 
 made up of grits and fine conglomerates dipping at 55° to N. 50° E. 
 
 In Black Rock Creek, near Selection 1450, a vertical seam of inferior coal, two 
 feet three inches in thickness, is intruded into by a sheet of greyish diorite. The coal 
 is overlaid by buff-coloured shales. 
 
 Sandstones, grits, and shales, with sheets of diorite and dolerite, are seen at 
 intervals in the low hills between Black Rock and Alligator Creeks. 
 
 “The stratiform series of volcanic rocks upon the uneven surface of which some 
 of the sedimentary series were laid down,” says Mr. Maitland, “ are best developed on 
 the northern side of the Pioneer River, where they cover a considerable tract of country. 
 In no place was their base seen, and consequently no estimate of their thickness could 
 be made. The rocks forming the series are diorites and basalts, with breccias and 
 agglomerates. Nowhere do these rocks form any conspicuous feature, occupying, as 
 they do, the rounded knobs on the lower ground.”’* 
 
 J. 
 
 
 
 The greater part of the details given in this chapter are taken from Mr. A, Gibb Maitland’s Report 
 on the Mackay District. Brisbane: by Authority: 1889. 
 Note To Pace 21.—Since this page was in print, the Warden has reported (31st December, 1891) 
 that, in his opinion, the Last Call Mine, Cloncurry, must have been “ salted,” 
 
 ? 
 
 q 
 
 
 
CHAPTER XIV. 
 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 THE MIDDLE BOWEN FORMATION IN THE TYPE DISTRICT. 
 
 Tue trappean rocks lying on the Lower Formation have been covered by sedimentary 
 rocks, and the sedimentary and igneous rocks have been disturbed from their original 
 horizontal position at the same time and in the same degree. ‘The activity of the 
 voleanic forces must have been considerably diminished, as neither lava-form nor ashy 
 beds occur higher in the series. But that the voleanic activity did not cease for a long 
 time is proved by the fact that molten rocks of the dolerite type were again and again 
 injected along lines of weakness in the sedimentary rocks. 
 
 Following the right bank of the Bowen River from Biralee Station upwards, 
 after traversing a basaltic plain for about three miles, a wall of white gritty sandstone, 
 running N. 20° W. to S. 20° E., crosses the path. This sandstone is the lowest bed of 
 the Middle Series. Its outcrop can be easily followed down the bank into the river, 
 where the sandstone is seen to overlie, apparently without any break, a felspathic 
 sandstone, which, in its turn, rests on the surface of a bed of porphyrite. The porphyrite 
 and sandstone both dip E. 20° N. at a low angle. This is the only place where the base 
 of the Middle Series is unequivocally visible. In other places—e.g., Pelican Creek, 
 Coral Creek, and the Bowen River two miles above Beasley’s (ruined) Public-house— 
 the sedimentary and igneous rocks may be observed in close juxtaposition; but there 
 are reasons for believing them to be separated in these places by a line of fault, and that 
 neither the highest members of the one series nor the lowest of the other are seen at the 
 points of junction. ~ About three miles above the old crossing at Beasley’s, a sandstone 
 bed crosses the Bowen River, dipping at 35° to S.W. This bed forms a conspicuous 
 cliff known as “ The Wall,” which is traceable for miles to the south-east, Itis evidently 
 tilted by the fault which divides the coalfield from the metamorphic rocks to the north- 
 east. 
 
 Up to a point midway between the mouths of Rosella and Parrot Creeks, the 
 Marine Series occupies the bed of the Bowen River. After plotting the observed 
 dips of the strata, I estimated the total thickness at 1,848 feet. It will be seen from 
 the Geological Map that the area occupied by the Middle Series is much greater at the 
 north-west end of the field than on the eastern side. This is accounted for by the 
 comparatively high dip of the strata in the latter region. 
 
 The Middle Series is made up of alternations of grey and yellow sandstones and 
 blue and grey shales, with here and there bands of reddish ferruginous, probably once 
 calcareous, sandstones, sometimes varying to impure sandy ironstones. ‘T'wo seams of 
 coal (besides some carbonaceous beds hardly deserving the name of coal) occur in this 
 series. These seams have been named the Garrick and the Kennedy. Other seams of 
 coal have been met with in a bore to be afterwards referred to. Near the top of the 
 series, black shales, highly impregnated with alum, are abundant. 
 
 A few beds of conglomerate are met with, chiefly in the lower part of the series. 
 The pebbles are generally of granite, slate, schist, quartzite, and other metamorphic and 
 

 
 151 
 
 plutonic rocks, with a few of porphyrite. The pebbles, which are not always well 
 rounded, have a remarkable tendency to arrange themselves in groups in some of the 
 conglomeratic sandstone beds—a disposition which may possibly be owing to their 
 having been dropped in heaps from the floating roots of trees, but much more likely to 
 their having been dropped from floating ground-ice. Large isolated boulders of granite, 
 &e., which could hardly have been brought to their present positions except by glacial 
 action, occur here and there in the midst of strata of fine sandy or muddy material. 
 Portions of the trunks of coniferous trees are occasionally found lying horizontally in 
 the strata. 
 
 The bands of ferruginous sandstone are storehouses of marine fossils, which 
 occur also, though more sparingly, in the shales and grey sandstones. In the latter the 
 shells are almost always calcareous, and contrast strongly with the siliceous and 
 felspathic sandstone matrix. In the ferruginous sandstones, on the other hand, the 
 fossils are always in the form of casts. About fifty feet of pebbly sandstone strata on 
 Stonehumpy Creek are absolutely crammed with shells, especially Strophalosia Olarkez, 
 Eth. Another sandstone bed, at least one hundred feet thick, in the Bowen River, 
 about two and a quarter miles above the old crossing at Beasley’s, is also full of 
 Strophalosia Clarkei. Derbyia senilis, Phillips, is abundant on Coral Creek; and on 
 Pelican Creek, one mile above the Bowen and Sonoma Road, and near the Diamond 
 Drill Bore. Productus, Spirifera, and Martinia are common throughout the whole 
 series. The shales and grey sandstones are frequently pierced by rootlets in the 
 position of growth. The marine shells prove that the strata were mainly deposited 
 by a sea, of which the Clarke Range formed the eastern shore; while the upright 
 rootlets in the grey sandstones and shales indicate the occasional appearance of land 
 surfaces. 
 
 Near the base of the series, especially in Coral and Pelican Creeks near Sonoma 
 Station, besides Mollusca of the usual types, Actinozoa and Polyzoa occur in great 
 abundance. Of the former, Stenopora Jackii, Nich. and Eth. fil., is the most common. 
 Of the latter, Protoretepora ampla, Lonsd., P. Koninekii, Eth. junr., and Fenestella 
 fossula, Lonsd., are all equally common. In one specimen in the Geological Survey 
 Museum Glossopteris occurs in the same slab with Protoretepora ampla. One bed in 
 Pelican Creek half-a-mile above the road from Bowen to Sonoma, consisting of a sandy 
 ferruginous limestone, is a mass of the coral Stenopora Leichhardtii, Nich. and Eth. fil. 
 This fossil is remarkable for its brilliant red colour. 
 
 A large collection of fossils (Mollusca) from the Middle Series near Blenheim has 
 been presented to the Geological Survey Museum by Mr. R. T. Barker, of Eungella. 
 These still remain to be examined in detail. 
 
 About two hundred and seventy five feet above the base of the series is the 
 Garrick Coal-seam, the outcrop of which is seen on Pelican Creek. Another seam, 
 named the Kennedy, is believed to overlie the Garrick, but, as the two cliff-sections are 
 not continuous, this cannot be stated with certainty. 
 
 In the bed of the river there can be seen in dry seasons the outcrop of a seam of 
 coal about twenty feet beneath the outcrop of the Garrick Seam which is seen in the cliff 
 above. The seam in the river may possibly be the Kennedy Seam, in which case there 
 must be a fault, with a downthrow to the west, between the two cliffs containing the 
 outcrops of the Kennedy and Garrick Seams. As the seam in the river was not met 
 with in the bore, afterwards to be referred to, it must, if its place is below the Garrick 
 Seam, either have thinned out in the half-mile which intervenes between the outcrop of 
 
 the Garrick Seam and the bore, or its absence from the latter may be explained by a 
 small fault. 
 
152 
 
 The following is a section of the seam seen in the bed of the river :— 
 
 Ft. in. 
 Soft yellow sandstone wee oe nae mee ars BS sian aes 
 Coal oe i ai 0 4 
 Clay Oat: 
 Coal 0 10 
 Clay On 1 
 Coal 0 9 
 Fireclay 1 8 
 
 The coal has a specific gravity of L 37 and is free of pyrites. It was used for the 
 pumping engine attached to the bore. Its analysis is:— 
 Moisture .. doc on sot 300 Aste cae go Pe 
 Volatile hydrocarbons es See a san oa ae OL 
 Fixed carbon... 3 03 she a 500 we. 59°09 
 Ash res 560 +e oe dot 506 sat ww. =16°04 
 
 
 
 100:00 
 
 The section of the cliff showing the Kennedy Seam is as follows :— 
 Ft. 1 
 Soft white flaggy sandstones and shaly alte fe aa eee 
 
 Talus, concealing about... z si cm oan a metib 
 
 Dark-blue shales 
 
 Soft grey sandstone .. 8 
 
 Gritty white siliceous sandstone oe 
 
 Dark-blue shales 
 
 Coal ... 
 
 Dark-blue shales 
 
 Coal, Kennedy Seam - 
 
 White fine-grained soft clayey sandstone, with upright rootlets 
 
 Soft yellow sandstone ~ - ix: wes ry, 
 
 Sandy shale ... , 
 
 Soft yellowish sandstone 
 
 Shales, with a line of large ironstone nodules 
 
 White sandstone, in bands of about 8 inches thick 
 
 Shales.. : .. 
 
 ae ellowish amigas 
 
 The Kennedy Seam, as seen at its outcrop, i is made up of fine lamine of varying 
 
 purity and lustre, some of the laminz being mere carbonaceous clay, and others good 
 coal. The coal burns with difficulty, leaving a scarcely diminished bulk of reddish 
 
 AH MamonwnmnnrrHooonwon 
 S1S.0°O OS CS OO LS B09 IO SS OOF 
 
 shaly ash. It splits readily along the bedding-planes, and at right angles to these - 
 
 along numerous joints, and is very friable. It does not take a polish under the knife, 
 but breaks up into minute cubes. The powder is ink-black. Its specific gravity is 
 1°463. 
 ANALYSIS. 
 Water... F ve cite eee = ave Fed Be 
 Volatile Be \roearhons abe ir re 06 ie oot, Co btSHL 
 
 Fixed carbon - 42°79 
 Ash (light brown) } A bright, hard coke, 57:07 per cent. { 14:28 
 
 100°00 
 The cliff-section showing the Garrick Seam is as follows :— Ft. in. 
 Thick-bedded yellow sandstone, with Kdmondia a pat (oc et 
 Soft flaggy and shaly grey sandstone... ce sf ee ee aL 
 Impure sandy ironstone, weathered sek = gue (aaa) 
 Soft fine-grained laminated grey shale, weathering yellowish” . 6 0 
 Coal, Garrick Seam .. xe es eget ie Pir 6 
 Soft grey shaly sandstone, Rit (eparse) rootlets 5 0 
 
 
 
 —_— ae 
 
PD pa ot: 
 PM oe nara A me hi 
 
 
 
1 iy 
 a 
 
 5) 9 
 
 by 
 vi 
 
 
 

 
 ee a 
 
 158 
 
 The Garrick Seam is seen in the cliff on the left bank of Pelican Creek. For 
 about a third of this distance an intrusive sheet of ‘“‘white trap” is seen cutting into the 
 seam and rendering it locally useless, but the remainder of the outcrop is undisturbed. 
 
 The Garrick Seam at its outcrop, and where it is not burnt by the white trap, 
 shows layers of shining coal alternating with layers of dark coaly shale. It burns with 
 difficulty and leaves a good deal of brown ash. The joints are coated with sulphur and 
 alum, The coal is moderately firm. It takes a feeble polish under the knife, with a 
 deep black lustre. The powder is lamp-black. The specific gravity is 1°456. 
 
 
 
 ANALYSIS. 
 Water ... ae 4 os ee oe ee dies 
 Volatile ir arocarbona ose i Ae ae ais a ov ap 
 Fixed carbon 46°60 
 Ash (grey) } A bright, hard coke, 63°52 per cent. { 16°92 
 100°00 
 
 Near the bottom of the seam a light, feebly lustrous, non-soiling coal occurs in 
 nodules of three or four inches in diameter. They burn well. It would appear that 
 in the formation of these concretions some of the earthy impurities have been rejected. 
 Their specific gravity is 1402. An analysis of one of these nodules gave— 
 
 
 
 Water... a as ay hi spe ee Rte) 
 Volatile iv icctar bons ans 30 ons Shc vas Pee LoIoo 
 Fixed carb 67°58 
 ae ne am Spongy coke, very hard, 79°12 per cent. 1 1154 
 
 100:00 
 
 A bore was sunk by the Government through the Garrick Seam to the base of 
 the Middle Series in 1885. In company with Mr. Hester, the Engineer in charge of the 
 bore, I examined the cores in August of that year, and compiled the foliowing section, 
 It is important as giving a continuous section of the lowest 339 feet of the Middle 
 Series. 
 
 Section or No. 1 Bors, Penican Creex. 
 
 Thickness. Depth. 
 
 , Ft. In. Ft. In. 
 
 Loam and clay ... oh ae oe + 2 Ae 0 a 4 0 
 
 Loose rock a »s ear #0 or et 
 
 Fine-grained buff micaceous Prandatene fcoseye 
 
 fissure and large opening at 25 feet... Pate nt 25 0 
 Fine-grained micaceous sandstone, buff, graduating 
 
 downward into white (fissure) ... we var ade O : 69 O 
 
 Mud- “seam, hardening downward into black 
 micaceous shale (no core) ‘ 
 Fine-grained dark-grey micaceous sandstone, with 
 
 i 
 o 
 ~w 
 o 
 o 
 
 plant-impressions .. PP te se 0 6 70 6 
 Dark sandy shale OG oes deli) 
 Soft clay... Oia (Mea! 
 ad Soft coal (no core) 1 0 fepe al 
 ont 5 Burnt coal (a) . . 176 coms 
 ES Mixed white clay and prrites 0 03 13.7% 
 So Burnt coal ae 2 43 76 0 
 Fireclay (no core) 01 TO) 1 
 Fine-grained blue-grey micaceous sendetone. ith 
 streaks of carbonaceous shale .,., te 6 11 83 0 
 White gritty sandstone, with streaks of micaceous 
 _and carbonaceous shale ... as We “40 87 0 
 
154 
 
 Section or No. 1 Bors, Petican CreEK—continued. 
 Thickness. 
 Ft. 
 
 White sandstone, alternately fine and coarse grained, 
 with bands of carbonaceous and micaceous shale 
 
 Blue shale, with layers of sandstone and streaks of 
 carbonaceous shale 
 
 Very hard conglomerate 
 
 White freestone 
 
 Coaly streak 
 
 White freestone, with ceRionel pachonaten aa films 
 and plant-impressions 
 
 Dark-blue carbonaceous shales, ostasionally sandy 
 
 Gritty freestone (admirable scythestone), with a few 
 carbonaceous streaks 
 
 Fine-grained grey shaly sandstone ... 
 
 Clay film 
 
 Burnt coal (a) ... 
 
 Clay 
 
 Coal Galena on no core, only emall fa agment 
 preserved ... 
 
 Clay vit 
 
 Burnt coal (0) 
 
 White trap 
 
 Dolerite ... - ase 
 
 Sandstone and conglomerate Aa 
 
 Coal (c) . Us a5 
 
 Fine- eraiped Finish: gee “itis Pees we 
 
 Coaly streak... + 
 
 Fine-grained bluish- nie joel sandstone a ' 
 
 Coal, good (according to Mr. Hester)—none rel 
 
 White gritty sandstone 
 
 Coarse gritty sandstone, occasionally -aatike and 
 with a few dark streaks ... é 
 
 Alternate coarse and fine gritty sandstone, with s a 
 few dark streaks ... 
 
 Coal (bright and ieee according to Mr. 
 Hester)—none saved 
 
 Dark-blue shale and burnt coal, occasionally shaly 
 and full of pyrites (d) 
 
 White trap, passing downward into dolerite 
 
 Dolerite ... 
 
 White trap, re ml sid 
 
 Blue-black shale, math coal-streaks and eiper es 
 
 Black shale, full of plant-remains 
 
 Dolerite, involving a little coal 
 
 Burnt coal (a) 
 
 White trap and burnt coal ed 
 
 Calcite cavity, with pyrites crystals... 
 
 Burnt coal 
 
 White trap 
 
 Burnt coal (a) . Spe 
 
 Black shale, with, Classen tert is 
 
 Coal (good) (e) . 4 sei 
 
 Coaly shale, with much carbonate of lime ue 
 
 24, 
 
 11 
 
 Oo 
 
 OMOKHOOOCOCOFRN AB OO bb 
 
 = =) 
 
 in. 
 
 0 
 
 — 
 oo or Coo wWo 
 tole bi 
 
 HO 
 
 peer 
 ww FPrEPrOOMmMOrF © 
 
 tol polH Sie 
 
 nr 
 
 ROIQDMwmBwooWdwnwonAnraooododaw 
 
 Depth. 
 
 Ft. 
 
 93 
 
 110 
 110 
 115 
 115 
 
 150 
 171 
 
 181 
 185 
 
 187 
 
 187 
 
 188 
 188 
 190 
 191 
 192 
 192 
 196 
 208 
 
 216 
 
 216 
 251 
 
 275 
 
 286 
 
 288 
 289 
 294, 
 298 
 303 
 305 
 306 
 307 
 307 
 307 
 307 
 307 
 309 
 309 
 315 
 315 
 
 o 
 
 Sowo 
 
 rer 
 
 es 
 
 — 
 
 OrFPOWNFEPNH 
 
 o ono 
 
 oO 
 
 qo 
 
 bo|h 
 
 SS DDO RMROCOOOOS 
 | nol bole 
 
 it) 
 
 oO 
 

 
 155 
 
 Section oF No. 1 Bort, Petican CreEeK—continued. 
 
 Thickness. Depth. 
 Ft. in. Gaay 
 Fine breccia of angular fragments of hard white 
 clay and black shale, with coaly plant-streaks 1 3 ae 316 7 
 Black shale, full of carbonised plant-remains, with 
 coaly streaks ae 0.9 317 4 
 Fine breccia of angular fragments of hard white 
 clay and black shale with coaly plant-streaks.. 1 3 318 7 
 Black shales, with coaly streaks a De eA) 321 7 
 Coal (good) ve . One2 321 9 
 Black shale, with one poenle and oeoasional 
 brecciated parts as above ¥ 3 3 325 0 
 
 Coal (only borings, drillings, and about 4- eeaee of 
 
 core preserv ei The drillings show coal of 
 
 good quality mixed with shale; the }-inch of 
 
 core is good coal ... age [05.6 ay 325 6 
 Black shale, with coaly streaks and carbonised 
 
 plants and occasional fragments of hardened 
 
 clay ; ed UKE 327 0 
 Black site aie. with carbonised plant -remains,. 2 0 329 O 
 Coal (good), $-inch of core Orel 329 1 
 Black shale, with carbonised set remains 0 1L 330 0 
 Coal (good), about 1 inch of core 0 6 330 6 
 Black shale, with carbonised plant-remains ae 2 Q 332 6 
 Fine breccia of angular fragments of hard white 
 
 clay and black shale, Paik coaly streaks 4 6 337 0 
 Dark-blue shale 0 6 337 6 
 Breccia, as above O 6 338 O 
 Black shale : 0 2 338 2 
 Dolerite, passing upwar da aa derawerde into 
 
 white trap .. T10 340 O 
 Black shale, with carbonised pieneer remains 2 2 342 2 
 Breccia, as above, with coaly streaks 1h ail 343 3 
 Coal layer : 0 5 343 8 
 Black shale, with earboutsed plant-re remains 0 8 344 4 
 No record : , 6 8 
 Black carbonaceous hale sing he praingd lace 
 
 sandstone, at a ‘aa 351 O 
 Amy gdaloidal araliceie with preatita and. calespar 39 6 Se 390 6 
 
 The burnt coals (a), at 72 feet 1 inch, 185 feet, 306 feet 6 inches, and 307 feet 
 103 inches, were represented by a hard, heavy, earthy coke, full of pyrites and vertical 
 veins of carbonate of lime. This coke decrepitates and flies off a charcoal fire. It 
 leaves a dull-black stcne after being heated to redness. 
 
 The burnt coal (4) at 188 feet 2 inches was represented only by drillings and 
 small chips. From the drillings it appeared to be partly a slaty coal and partly a dark 
 pyritous shale with coaly films. The bottom of the seam had an irregular and typically 
 intrusive junction with the ‘white trap,” as in Pl. 51, fig. 1. 
 
 The coal-seam (¢) at 192 feet 9 inches was only represented by the drillings, and 
 appeared from them to be a seam of alternate good coal and shale. The drillings 
 burned fairly well in the forge. 
 
 The bottom of the coaly seam (d), struck at 286 feet 3 inches, was penetrated by 
 intrusive “white trap.” 
 
156 
 
 The coal (e), at 309 feet 63 inches, was the only seam of workable thickness and 
 quality met with in the bore. The thickness of the seam, as reported by Mr. Hester, is 
 5 feet 54 inches; but this was only represented by about 1 Ib. of fragments, it having 
 been found impossible to extract a core. The following is an analysis of this seam:— 
 
 
 
 Per cent. 
 Moisture ... oa ves ae nt any ir ek yous 
 Volatile hydrocarbons ... ose set ae see a 20 20 
 Fixed carbon ... a sad ep a, 5A ren oy GY / 
 Ash os; Ge ar ae ae ee Fry na OB: 
 
 100°00 
 
 Specific gravity, 1°56. 
 
 The coal swells a little on ignition, but falls away to a white ash without stirring. 
 The powder is black. The coke swells a good deal, but is bright and firm. The seam 
 would make a fair furnace coal, although the quantity of ash is certainly high. 
 
 In the bore, as in natural sections, the white trap graduates, as it recedes 
 from the carbonaceous strata, into dolerite, although in natural sections it might be 
 taken for a weathered acidic igneous rock. The junctions of the white trap and coal 
 seen in the cores are most interesting and instructive. It would appear in some cases 
 as if the coal had intruded into the white trap rather than the converse. The sample 
 drawn in PI. 51, fig. 1, shows this deceptive appearance very well. In PI. 51, fig. 2, 
 threads of coal penetrate the white trap like veins. In Pl. 51, fig. 3, the white trap 
 occurs in irregular masses throughout the coal, these irregular masses being probably 
 connected in the interior of the core, although they appear isolated in section. The 
 molten rock appears to have, so to speak, eaten its way into the coal-seam and ultimately 
 consolidated, while unconsumed fragments and films of the coal remained involved in 
 its mass. The conversion of dolerite into white trap where it comes in contact 
 with carbonaceous rocks has frequently been noted in the coalfields of Scotland and 
 elsewhere. 
 
 J. 
 

 
 CHAPTER XY. 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 THE MIDDLE BOWEN FORMATION OUTSIDE OF THE TYPE DISTRICT, 
 
 Inctupine Neso, Mackay, BANANA Creek, Cracow Crirrex, Nogoa River, SPRINGSURE, 
 Logan Downs, and Roper CREEK. 
 
 In the neighbourhood of Mackay generally the Permo-Carboniferous rocks are 
 well represented. It will be convenient to give in this place a short account of the 
 Middle or Marine Formation of the Bowen River as developed in the Nebo District. 
 
 Three miles south-west of Mount Britton Township, on a ridge near Mr. 
 Richards’ Selection, some beds of ferruginous, and in part calcareous, sandstones are 
 seen dipping to the north-west. They are full of fossils of the type of the Middle 
 or Marine Series. These are casts of numerous shells, &c., of which I made a large 
 collection in 1887. The collection has been supplemented by Mr. A. L. Morisset, Mr. 
 R. Hull, and others. Among the fossils identified by my Colleague are— 
 
 Platycrinus ? nux, Eth. fil., Pl. 38, fig. 3. 
 
 Spirifera, sp. ind., Pl. 88, figs. 4, 6. 
 
 S. Strzeleckii, De Kon., Pl. 10, fig. 37. 
 
 Spiriferina duodecemcostata, McCoy, Pl. 44, fig. 12. 
 
 Martinia subradiata, G. B. Sowerby, Pl. 11, fig. 14. 
 
 Martiniopsis Darwinii, Morris, Pl. 9, figs. 18, 14; Pl. 39, figs. 5, 7. 
 
 Productus cora, D’Orb., Pl. 12, fig. 14; Pl. 18, fig. 1; Pl. 38, fig. 11. 
 
 P. brachytherus, G. Sowerby, Pl. 12, figs. 10-18; Pl. 18, fig. 5; Pl. 44, 
 fig. 14. 
 
 P. subquadratus, Morris, Pl. 38, figs. 7-10; Pl. 40, fig. 5. 
 
 P., sp. ind. (e), Pl. 37, fig. 18. 
 
 Chonetes, sp. ind. (d), Pl. 87, fig. 19. 
 
 Deltopecten illawarrensis, Morris, Pl. 41, fig. 3; Pl. 44, fig. 2. 
 
 Modiomorpha mytiliformis, Eth. fil., Pl. 14, fig. 5; Pl. 40, fig. 4. 
 
 Orthoceras, sp., Pl. 15, fig. 1. 
 
 A species of Fenestella is also common. 
 
 The track from Mount Britton to Eungella passes by the Moonlight Diggings, 
 east of Mount Robert and west of ‘The Stalk.”* Just beyond Mount Robert, fossils 
 of the same species as those at Richards’ were seen on the road. 
 
 The Middle Formation in the Mackay District is described by Mr. Maitland, in 
 his Annual Report for 1889, as ‘‘made up mainly of sandstones and shales, and 
 ferruginous sandstones, with occasional contemporaneous and intrusive sheets of dioritic 
 rock.” A few seams of coal occur among these beds. 
 
 On Banana Creek, a tributary of the Dawson (Lat. 24° 30’, Long. 150°), a con- 
 siderable addition has been made to the fauna of the Middle Formation by the labours 
 of Mr. C. W. de Vis, Mr. H. Mackay, and the late Mr. James Smith. These are— 
 
 Terebratula sacculus, Martin. 
 Spirifera lata, McCoy. 
 
 * See Runs Map of Leichhardt District and Runs Map of North and South Kennedy, sheet 2, 
 
158 
 
 Martiniopsis ? subradiata, G. B. Sby. 
 Strophalosia Gerardi, King. 
 
 Clarkei, Eth. 
 Modiomorpha mytiliformis, Eth. fil. 
 Chenomya Etheridget, De Koninck. 
 C. carinata, Eth. fil. 
 
 Mourlonia? coniformis, Eth. fil. 
 Bellerophon stanvellensis, Eth. fil. 
 Porcellia Pearsi, Eth. fil. 
 
 From Cracow Creek (south of Boolburra, Central Railway), on the Dawson 
 River, Mr. R. Etheridge, F.R.S., described * Chonetes cracowensis, Eth., and Pleuro- 
 tomaria (Platyschisma) rotunda, Eth. The beds yielding these fossils may be 
 presumed to belong to the Middle Formation. 
 
 From a locality described as “‘ Weelwondongara Creek, Nogoa River,” which I am 
 unable to identify, but which is probably on Wealwandangie squatting block, south of 
 Springsure, the same Author described + Productus or Strophalosia (Pl. 18, figs. 4, 
 4a) (Strophalosia Clarket, Eth.) This Brachiopod, as has already been seen, is very 
 characteristic of the Middle or Marine Formation. 
 
 Mr. Smith, shortly before his death, forwarded, from the neighbourhood of 
 Springsure, some Crinoid stems, and undoubted specimens of Strophalosia Clarkei, the 
 latter, as has already been seen, being a characteristic fossil of the Middle Formation. 
 
 Mr. Rands records in his ‘“ Report on Clermont” that, on Logan Downs Run, 
 forty miles north-north-east of Clermont, on the range west of Mount Rankin, Mr. 
 Rogers-Harrison found ‘ Cyathophyllum (two species), Strophalosia Clarkei, Productus, 
 probably P. brachytherus, and Arca?” Probably these beds belong to the Middle 
 Formation. 
 
 Daintree’s Paper on the “ Geology of Queensland” ¢ contains a list of fossils 
 identified by Mr. R. Etheridge, F.R.S., “from the head of Roper Creek and the Bowen 
 River,” all characteristic of the Middle Bowen River Beds. It is strange that Daintree, 
 of all men, should have mixed up fossils from different localities so that it is impossible 
 to say which was which; but we may take it for granted that somewhere in the neigh- 
 bourhood of Gordon Downs representatives of the Middle Bowen Series occur. The 
 Roper Creek referred to is probably ‘ Little Roper’s Creek,’ a tributary of Sandy or 
 Campbell’s Creek, which will be found on the map between the 22nd and 28rd Parallels 
 of Latitude and the Meridians of 148 and 149. Daintree’s Paper also contains (p. 283) 
 a list of apparently Cretaceous fossils from ‘‘ Gordon Downs, at the head of Roper 
 Creek,” sent by the Revd. W. B. Clarke to Mr. R. Etheridge, F.R.S. The words “at the 
 head of Roper Creek” are here probably inserted by mistake. There is a station named 
 Gordon Downs near Roma, which is a Cretaceous locality. 
 
 J. 
 
 
 
 
 
 
 
 * Quart. Journ. Geol. Soc. Lond., xxviii., pp. 336, 337. 
 + Loc. cit., p. 334. 
 £ Quart. Journ. Geol. Soc., xxviii., p. 286. 
 
CHAPTER XVI. 
 
 THE PERMO-CARBONIFEROUS SYSTEM —continued. 
 
 LIFE OF THE MIDDLE BOWEN FORMATION. 
 
 Tue following is a complete List of the Fossils identified or admitted by my Colleague 
 from this formation in all the localities where it occurs :— 
 
 Sphenopteris lobifolia, Morris. 
 Glossopteris Browniana, Brong. 
 2 linearis, McCoy. 
 sh ampla, Dana ? 
 Coniferous wood. 
 Stenopora australis, Nich. and Eth. fil. 
 ? Leichhardtii, N. and E., fil. 
 - Jackii, N. and E. fil. 
 Platycrinus ? nux, Eth. fil. 
 Crinoid stems. 
 Mesoblastus ? australis, Eth. fil. 
 Fenestella fossula, Lonsd. 
 
 Protoretepora ampla, var. Woodsii, Eth. 
 
 Protoretepora ampla, var. Koninckit, Eth. 
 
 fil. 
 Terebratula cymbeformis, Morris. 
 Dielasma sacculus, Martin, var. 
 Spirifera striata, Martin ? 
 
 - convoluta, Phill. 
 
 = lata, McCoy. 
 
 s Clarkei, De Kon. 
 
 7 trigonalis, Martin. 
 - sp. ind. (6), Pl. 88, figs. 4-6. 
 a tasmaniensis, Morris. 
 
 5 Stokesii, Konig. 
 
 a Strzleckit, de Kon. ? 
 Spiriferina duodecemcostata, McCoy. 
 Martiniopsis ? subradiata, G. B. Sby. 
 
 9 Darwinii, Morris. 
 
 Derbyia senilis, Phill. 
 Productus cora, D’Orb. 
 
 * brachytherus, G. Sow. 
 
 - subquadratus, Morris. 
 
 5 sp. ind. (e), Pl. 37, fig. 18. 
 Strophalosia Clarkei, Eth. 
 
 3 Gerardi, King. 
 Chonetes cracowensis, Eth. 
 
 “ sp. ind. (d), Pl. 87, fig. 19. 
 
 Aviculopecten subquinquelineatus, McCoy. 
 
 4s limeformis, Morris. 
 Deltopecten illawarrensis, Morris. 
 Merismopteria macroptera, Morris. 
 Modiomorpha mytiliformis, Eth. fil. 
 Solemya Edelfelti, Eth. fil. 
 Astartila cytherea, Dana. 
 Chenomya ? Etheridget, De Kon. 
 
 4s carinata, Eth. fil. 
 
 ce acuta, Eth. 
 
 bowenensis, Eth. fil. 
 Pachydomus globosus. 
 Meonia carinata, Mor. 
 
 » recta, Dana. 
 
 Platyschisma rotunda, Eth. 
 Mourlonia ? coniformis, Eth. fil. 
 Bellerophon stanvellensis, Eth. fil. 
 Porcellia Pearsi, Eth. fil. 
 Orthoceras, sp. 
 Goniatites micromphalus, Morris. 
 
 Of the above, Glossopteris ampla?, Stenopora australis, 8S. Leichhardtii, S. Tackii, 
 Platycrinus? nux, Protoretepora ampla, var.Woodsii, P. ampla, var. Koninchii, Terebratula 
 cymbaformis, Dielasma sacculus, Spirifera striata, S. convoluta, S. Clarkei, S. sp. ind. (b), 
 Spiriferina duodecemcostata, Productus, sp. ind. (e), Strophalosia Clarkei, 8S. Gerardi, 
 Chonetes, sp. ind. (d), Aviculopecten subquinquelineatus, Deltopecten illawarrensis, Meris- 
 mopteria macroptera, Modiomorpha mytiliformis, Solemya Edelfelti, Astartila cytherea, 
 Chenomya ? carinata, C.? acuta, OC. ? bowenensis, Pachydomus globosus, Meonia carinata, 
 
160 
 
 M. recta, Mourlonia ? coniformis, and Goniatites micromphalus occur only in the Middle 
 Bowen Formation and are not known from any of the other subdivisions of the Permo- 
 Carboniferous. 
 
 Chonetes cracowensis, Porcellia Pearsi, and Orthoceras, sp., are common to the 
 Gympie, Star, and Middle Bowen Formations. 
 
 Fenestella fossula, Spirifera lata, S. trigonalis, S. Stokesii, S. Strzleckii ?, 
 Martinia subradiata, M. Darwinti, Productus cora, P. brachytherus, P. sub- 
 quadratus, Aviculopecten limeformis ?, Ohanomya? Etheridgei?, Platyschisma rotunda, 
 and Bellerophon stanvellensis occur in the Middle Bowen and Gympie Formations, but 
 not in any of the other subdivisions of the Permo-Carboniferous. 
 
 Sphenopteris lobifolia, Glossopteris Browniana, G. linearis, and Derbyia senilis 
 occur both in the Middle and Upper Bowen Formations, but not in any of the other 
 subdivisions of the Permo-Carboniferous. 
 
 Productus brachytherus is common to the Gympie as well as to the Middle and 
 Upper Bowen Formations. 
 
 The following Genera are common to the Middle Bowen and Gympie Forma- 
 
 tions :— 
 Actinozoa: Stenopora. 
 Ponyzoa: Fenestella and Protoretepora. 
 Motivusca: Dielasma, Spirifera, Martiniopsis, Productus, Chonetes, Aviculo- 
 pecten, Modiomorpha, <Astartella, Chenomya, Mourlonia, Bellerophon, 
 Poreellia, Orthoceras, and Goniatites. 
 The following Genera are common to the Middle Bowen and Star Formations :— 
 Potyzoa: Fenestella. 
 Motiusca: Spirifera, Spiriferina, Chonetes, Porcellia, and Orthoceras. 
 The following Genera are common to the Middle and Upper Bowen Forma- 
 tions :— 
 
 Prantm: Sphenopteris and Glossopteris. 
 Mouiuscsa: Derbyia, Productus, and Goniatites. 
 
CHAPTER XVII. 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 THE UPPER BOWEN FORMATION IN THE TYPE DISTRICT. 
 
 THE uppermost beds of the Middle Formation dip at a comparatively low angle, and 
 conformably, to the east, beneath the lowest beds of the Upper Formation in the Bowen 
 River, near the mouth of Cockatoo Creek. The dip gradually becomes flatter for about 
 eight miles up the river, till, at the mouth of Jack’s Creek, the strata are horizontal. 
 Thence they gradually rise for about five miles further up the river, when a bed of grey 
 sandstone, dipping at 50° to S.W., and full of Strophalosia Clarkei, Eth., is seen crossing 
 the river. This sandstone, and the strata which succeed it for the next mile up the 
 river, all belong to the Middle Series. 
 
 To the north of the Bowen River, the Upper Formation comes directly in 
 contact, through the agency of a fault, with the older metamorphic rocks of the Clarke 
 Range, consisting here of quartzites, shales, greywackes, &e. 
 
 With the exception of the coal-seams the strata of the Upper Formation consist 
 almost entirely of grey shales and greenish-grey sandstones, which are occasionally 
 pebbly. The total thickness of the Upper Formation cannot be estimated, as its upper 
 beds are not seen; but from the lowest bed to the axis of a synclinal trough in Rosella 
 Creek there must be at least 1,000 feet of strata. 
 
 The Daintree Coal-Seam crops out in the bed of the Bowen River, about a quarter 
 of a mile below the mouth of Rosella Creek. Its position is evidently very near the 
 base of the Upper Series. Above the coal, a sheet of dolerite, about twenty-five feet 
 in thickness, occupies the bed of the river for one hundred yards. The lower portion 
 of the dolerite has been converted into white trap. Its actual base is concealed by a 
 talus, a gap of perhaps ten feet intervening between the dolerite and the underlying 
 strata. The following is the section, which dips to E.S.E. at 7°:— Be 
 
 in 
 Dolerite, the lower part white trap a on ie ce pene eao” 0 
 Gap—room for of a 
 
 ( Burnt coal, partly columnar somewhat coked i in part; veins and 
 pockets of white trap in upper part; concretions of ironstone 
 in vertical and horizontal joints; nodules of decomposed pyrites; 
 Glossopteris recognisable in parts 
 
 Black shale .., 
 
 Burnt coal 
 
 Black shale 
 
 Burnt coal... 
 
 Black shale ... 
 
 4 Burnt coal a 
 
 Bluish-grey shales ... ; 
 
 Stony burnt coal with alee plant. ake (d) aK 
 
 Light porous crumbling coal, with concretionary nodules ao better 
 coal (c) 
 
 Coaly shale 
 
 Light brownish- fee ented coal (some of the amine rather 
 oil-shale than coal), fair aie (0)... 
 
 Pluish-black shales ... Aa 
 
 (Good coal (a)... 
 
 
 
 
 
 
 
 OoOrooqoqoqooqoen 
 Onworqarewrn 
 
 Daintree Seam. 
 
 
 
 
 
 SS 
 bo © 
 
 
 
 onmn 
 wow oe 
 
162 
 
 Ft. in. 
 Dark-blue shales, with Phyllotheca, &c. (some lamin eat! say ... 10 O 
 Flaggy brown sandstone with plant-remains _... on wi er UeLU 
 Ironstone... ie Om 
 Bluish-grey shales : : Ls 
 Brown sandstone with pegenter: usr Et 0 3 
 Brown flaggy sandstone, with plant-remains - 1 6 
 Grey shales, with 13-inch band of good clayband ene ass 4 0 
 
 The coal from the seam marked (d) upwards has been destroyed by the igneous 
 rock, which wanders through it in the form of veins and “pockets,” renders it columnar, 
 and converts it partly into a kind of stony coke and partly into an earthy graphite. 
 The coal beneath is less injured, and the three-inch band marked (a) presents no visible 
 sign of having suffered from the heat radiated from the intrusive dolerite. 
 
 The band marked (a) is jet black and lustrous, with, however, some dull lamine. 
 It took fire easily and burned with a fierce heat, kine g, giving out much gas, and 
 leaving but little ash. The coal takes a polish under the knife. The powder has a 
 lead-black hue. The coal (at least at its weathered outcrop) has a tendency to break 
 up in right rhombic prisms. It has reticulating films of calcite in the joints. Its 
 specific gravity is 1°453. 
 
 ANALYSIS. 
 Water... ae ee sto $y Ps: eee OL 
 Volatile Redrocacbone on Be ans 5 an wo 20°02 
 Fixed carbon 2 ms ( Se nate so EB HAO) 
 ‘Ash (white) § COR 78°07 percent. 7 ee ay 
 
 
 
 100:00 
 
 The coke is tender, and swells unequally along the lamine. 
 
 The seam marked (0) is rather slaty at the bottom, with alternate dull and shining 
 lamine. This portion burned with difficulty and left a good deal of ash. The upper 
 portion of the seam took fire easily, crepitated loudly at first (probably from moisture), 
 emitted a good deal of gas, and then fell away leaving little ash except from some shaly 
 lamine. The purer layers of coal tend to split up in rectangular prisms, but are 
 otherwise very firm. The coal takes a fine brownish-black polish. Its powder is lamp- 
 
 black, 
 The upper part of the seam appears to be more homogeneous than the lower. 
 
 The laminated structure is equally distinct in both, but the lower appears to be more 
 broken up by shaly partings. 
 
 ’ ANALYSIS OF oP OF SEAM. 
 
 
 
 Water... nGe bon +f a dc we 244 
 Volatile hydrocarbows a ne oe sis es on oboe 
 Fixed carbon... Pe Soe aE wai < ww. 5740 
 Ash ee rs one nar ae oe an we 24°44 
 
 100°00 
 
 Specific gravity, 1°42. 
 
 ANALYSIS OF BoTTOM OF SEAM. 
 
 
 
 Water... aoe ay on D an ae 2.00 
 Volatile rake aire a0 les oct was St em GiOo 
 Fixed carbon ... ade cer at sag tee hoe BY A 
 Ash as Me tas a ene Ae Son PERE 
 
 100°00 
 
 Specific gravity, 1°513. 
 The bed marked (c) will hardly burn at all, and is in fact mere stone. 
 
163 
 
 The six-inch seam marked (d) is granular, like a mass of consolidated coal-dust. 
 It is feebly lustrous on some points of the surface. Soft portions dug into with a 
 knife or hammer take a bright black-lead lustre. It is, in fact, a sort of very earthy 
 black lead, with occasional fragments of a silky vegetable charcoal. It is interesting as 
 showing one of the stages in the alteration produced by the intrusive rock. It gives a 
 lamp-black powder, and has a specific gravity of 1551. 
 
 ANALYSIS. 
 Water... a Ap ae ner are ae ea OL 
 Volatile hydrocarbons ... ion eee aes ae a. 9,96 
 Fixed carbon ... : nr af Ran one ... 49°63 
 Ash eee eee eee eee eee eee eee oee 37°50 
 
 
 
 10000 
 
 The uppermost visible portion of the Daintree Seam (forty-three inches in 
 thickness) is in almost immediate contact with the overlying dolerite, and has, conse- 
 quently, suffered the extreme effects of the heat, having been rendered columnar 
 throughout, the columns having a transverse section of from half-an-inch to three 
 inches in diameter. The coal has been converted into a hard stony coke. It brightens 
 under the knife to a pale black-lead lustre. The powder is ink-black. Its specific 
 gravity is 1°779. 
 
 ANALYSIS. 
 Water... a see ico re an as eee ca 
 Volatile hydrocarbons ... a tes = ae are ah os 
 Fixed carbon... we as ad ee xe oe BLTo 
 Ash ne tee a oe sae ee a son the OY) 
 
 
 
 100°00 
 Up the Bowen River, about a mile and a-half north-east of the mouth of Rosella 
 Creek (near No. 19 Traverse Station), a little gully falls into the right bank of the 
 river. In one place the gully exposes twelve inches of coaly clay overlying six feet of 
 grey shale with carbonised plant-remains. A few yards down the gully, the following 
 strata are met with, lying horizontally :— 
 
 Ft. in. 
 Grey shales, with plant-remains aoe 
 Oil-shale (poor) e070 
 Coal (good), bituminous Ag 
 Black shale 0 4 
 Coal Noe OL 
 
 At the mouth of the gully the river falls over a sheet of dolerite, four feet thick, 
 which dips up-stream (east) at alow angle. On the opposite side of the river the 
 dolerite is seen to rest on a three-feet seam of burnt coal. These strata may be 
 estimated, on an average dip of 5°, to be about 480 feet above the position of the 
 Daintree Seam. 
 
 Probably on nearly the same horizon as the dolerite and strata in the Bowen 
 River last above referred to, are a number of sheets of intrusive dolerite, seen in 
 Rosella Creek, near Traverse Stations 1 and 2. About one hundred yards above No. 
 2 Station a dolerite sheet is seen, involving lumps of coal, and probably occupying the 
 place of a coal-seam. It dips to the south at 15°. 
 
 At No. 2 Traverse Station a sheet of intrusive dolerite, at least twenty feet thick, 
 crosses the creek, and ponds back a large waterhole. It dips to S.at 15°. At the 
 west side large blocks of burnt coal (one containing at least 1,000 cubic feet) are 
 
164 
 
 involved in the dolerite, while at the east side the section in Plate 51, fig. 4, remains to 
 attest the presence of a good coal-seam before the destroying mass of molten dolerite 
 forced its way among the beds. 
 
 In a little gully entering the right bank of Rosella Creek about half-a-mile from 
 its mouth, the following are seen lying horizontally. Their horizon cannot be very far 
 ‘above the Daintree Seam. 
 
 a 
 B 
 
 il 
 
 CO t=O OS Orr OSU 
 
 Dolerite (intrusive sheet), weathering spheroidally 
 
 Hardened blue shales (a) 
 
 Blue shales, with plants 
 
 Lenticular ironstone band ...° 
 
 Blue shales 
 
 Soft lenticular coal-seam 
 
 Ferruginous shales ... 
 
 Blue shales, with plants 
 
 Lenticular coal-seam 
 
 Lenticular ironstone seam ... 
 
 Blue shales vai cr oe os. ee 
 Lenticular mass of mineral eich (2) ae ; ; Sa 0 to 
 Blue shale, with plants, and very thin lenticular on and iponions seams 
 
 The juncture of the dolerite with the underlying blue shales, marked (a) in the 
 above section, is very remarkable, and shows that the shales were broken and torn by 
 the intrusion of the dolerite, as in Plate 51, fig. 5. 
 
 The mass of mineral pitch, (6) in the above section, appears to occupy an 
 irregular pocket in the shales, as shown in Plate 52, fig. 1. The origin of a cavity of 
 such a form is difficult to explain. 
 
 The next important coal-seam is named the MacArthur. It is seen in Jack’s 
 and MacArthur Creeks, on the right and left banks of the Bowen River respectively, 
 about eight miles above the mouth of Rosella Creek. Its position must be some 
 distance above that of the seam met with at No. 19 Traverse Station. 
 
 The MacArthur Seam on Jack’s Creek was prospected in 1875 in a “drive” by 
 the Bowen River Coal Association. The drive is said to have exposed a seam of coal 
 five feet in thickness, but worthless owing to the intrusion of a sheet of dolerite. 
 
 Near the mouth of the creek, about twenty feet of fine-grained grey argillaceous 
 sandstone bands, with plant-remains and grey shales, are cut out and overlaid by an 
 almost horizontal sheet of dolerite, which forms the upper half of the low hill in the 
 angle between the creek and the river. The dolerite weathers spheroidally. The nature 
 of the junction of the igneous and stratified rocks is sketched in Plate 52, fig. 2. 
 
 In MacArthur Creek, the MacArthur Seam and other strata are seen associated 
 with an intrusive dolerite as in the following section. The strata are horizontal :— 
 
 Ft. in, 
 Dolerite (on top of ape 1 Ae ie a a re Loan) 
 Burnt coal... : i: a bes aes at oe SO 
 Grey shale... =f sa _ are 5 
 Burnt coal, with shea layers i 
 Hard grey ferruginous sandstone ... 0 
 Burnt shaly coal da das e: ai seta ek 
 Grey-brown sandstone, with plant arrension a ed .. 3 in. to O 
 Grey shales ... ‘ te x2 wal ae vce 10 
 0 
 0 
 0 
 1 
 
 tol tole 
 
 CF AOSDSDODArP FEE WAO 
 
 LW) 
 
 Darker shales, with coaly lamine 
 
 Bituminous coal (tolerable) 
 
 Grey sandstone se 
 Crumbling coal, with es lamins, the coal lamin of fair quality, Hv ft. to 
 
 MacArthur Seam. 
 
 0 
 7 
 4, 
 7 
 7 
 3 
 9 
 I 
 1 
 9 
 
"oo 
 
 165 
 
 Ft, in, 
 Grey shaly fireclay, with rootlets 0 4 
 Darker shale . : ; Urs 
 Grey-brown fomedeiieae fegiia mass of Glossopteris is 0 4 
 Crumbling brown shale on a 0 5 
 Grey- oan ferruginous shale—a mass of Goweptore 0 3 
 Grey shale, with Glossopteris, &e. ve _ : fee 
 Grey sandstone, thin-bedded, with occasional plane ‘remains ... jae BOLD 
 
 Mr. A. C. Gregory reported as follows on a sample of the MacArthur Seam :— 
 
 Volatile in coking i ie sas wet bee Ne asi! 
 Fixed carbon mae sm 50 ee ee aie SOLO 
 Ash cx Ba is a ae ave Sf et (O26 
 
 100°0 
 
 Specific gravity, 1°67. 
 
 “The specimen appears to be injured by weather, and the coal will probably 
 improve at a greater depth. The percentage of ash is so high that the coal would be of 
 little value unless, by a careful selection from the best parts of the seam, the proportion 
 of ash should be lessened.’ Mr. Gregory had no opportunity of seeing the true cause 
 of the deterioration of the coal. 
 
 Near the head of Jack’s Creek the strata of the Upper Series are thrown down by a 
 fault against the older quartzites, greywackes, &c., of the Clarke Range, avd on approach- 
 ing the fault become nearly vertical. The strata Pane mainly of are shales, with thin 
 beds of hardened sandstone, and there are also a few beds of dark-blue crystalline lime- 
 stone, apparently unfossiliferous. These are the only limestones which I observed in the 
 Upper Series—at least in the type district. A dolerite dyke which has come up along 
 the bedding-planes of the shales and sandstones throws off a branch:at an angle of 45°, 
 which ‘“‘jumps’’ without being shifted by any fault, as sketched in Pl. 52, fig. 4. 
 
 For three miles up Jack’s Creek, above the level of the MacArthur Coal-Seam, 
 the strata are horizontal, so that their thickness is equal to the fall of the creek— 
 probably less than two hundred feet. The section is, however, very imperfect, the 
 rocks being only exposed at long intervals, except in the lower reaches of the creek. 
 These are invariably either grey shales or greenish-grey sandstone, which is sometimes 
 pebbly. About a mile north of the river a thickness of about fifty feet of greenish-grey 
 sandstone is seen, containing numerous large drifted coniferous trees. The trees, 
 which are silicified to a black flint, and sometimes opalised, occasionally retain some of 
 the branching roots. Fragmentary plant-remains, in a carbonised condition, are also 
 common. About half a-mile from the river the creek divides into two branches, both of 
 which show, for some distance up, section of the greenish-grey pebbly sandstone, with 
 silicified drifted trees. One tree measured thirty-one feet in length, and tapered from 
 twelve inches to three inches in diameter. 
 
 On the road from Havilah to Biralee, about a quarter of a mile west of Rosella 
 Creek, large silicified trees lie on the surface, in one of which I counted about thirty 
 rings of growth. Between the second and third Traverse Stations on Rosella Creek, 
 the following strata, which dip to S. at 15°, are seen on the right bank :— 
 
 Feet. 
 Bluish cross-bedded sandstone, weathering spheroidally, full of 
 carbonised and silicified plants, including coniferous trees. Large 
 unrounded boulders of metamorphic rock occur sporadically 
 throughout—about ee ra a ie the - = eS 
 Dolerite sheet ... Se Pee) 
 
 Grey shales and finely laminated cordateg awith Re bands of gaudy 
 ironstone ... ase ove ae wa) ewe eee rr ete 90 
 
166 
 
 The strata in the above section are believed to be identical with those which are 
 seen up Jack’s Creek. 
 
 About a hundred yards above No. 2 Traverse Station, on Rosella Creek, a 
 dolerite sheet is seen, involving lumps of coal, and probably occupying the position of 
 acoal-seam. It dips to S. at 15°. 
 
 Occupying apparently a position above the thick beds of sandstone above 
 referred to is the Havilah Coal-Seam, seen on the left bank of Rosella Creek, where the 
 paddock fence crosses. The following is the section, which has a slight dip to the 
 north-east :— 
 
 Ft. in. 
 Dolerite sheet on top of left bank. 
 
 Havilah Coal-Seam, burnt by “white trap” intruded along bedding 
 
 and rendered columnar, especially in upper part ... a ie, AOG 
 (About 200 yards up the ereek, the place of the coal is taken up by 
 
 the sheet of dolerite, which steals down into it.) 
 
 Dark and grey shales, with a two-feet bed of soft worthless coal in 
 the middle ot : ay ey ¥ Hee mraees UP a, 
 
 Greenish-grey sandstone, with trees. 
 Blue-grey shales, with plants, and lenticular seams of coal, and 
 
 calcareous bands, and bands of ironstone nodules (slight dip 
 to north-east). 
 
 The shales seen in the above section appear to die out up-stream, and a consider- 
 able thickness of greenish-grey sandstone takes their place. A quarter of a mile 
 higher the sandstone is pierced by a 33-feet dyke of dolerite, running E. 10° N., and 
 the lower coal-seam is again seen on the left bank. The Havilah Seam is burnt by 
 “white traps” intruded along the bedding, and is rendered columnar, especially in the 
 upper part. (See Sketch, Pl. 52, fig. 3.) 
 
 The Havilah Coal-Seam is not very far from the uppermost beds of the Upper 
 or Freshwater Series, as, after dipping to the south-east, the strata in a mile or 
 two begin to rise again in that direction. About a mile above the road from 
 Havilah to Byerwin, where it crosses Rosella Creek, there occur some beds of grey and 
 reddish ferruginous sandstones. In these beds marine fossils are numerous and well 
 preserved. Derbyia senilis, Phillips, is specially abundant. Loose blocks of silicified 
 wood, apparently from a higher bed which has been denuded, cover the shell beds. The 
 reappearance, high up in the Upper Series, which from its base upward has so far yielded 
 nothing but plant-remains, of strata charged with marine fossils, and these of species 
 which also occur in the Middle Series, is of the highest importance with reference to the 
 continuity of the two series. An analogous fact is the appearance of Glossopteris in 
 the Middle Series (even down to near the base, as evidenced by the Pelican Creek Bore), 
 associated with its characteristic marine fossils. 
 
 J. 
 
CHAPTER XVIII. 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 THE UPPER BOWEN FORMATION OUTSIDE OF THE TYPE DISTRICT, 
 
 Inotupina NuBo, Mackay, Lenten Downs, IsAacs anD Dawson Rivers, Cement Hiti, CLERMONT, 
 Bratr ATHOLE, AND DINNER CREEK, STANWELL. 
 On the right bank of Bee Creek, above its junction with Hail Creek, two shafts known 
 s “ Walker’s”’ were sunk about ten years ago. The shafts have tumbled in, and there 
 is no evidence to show whether they reached or cut through the strata exposed in the 
 bank of the creek, which are as follow :— 
 
 2 
 B 
 
 Dark shale with coaly streaks 
 Fireclay 
 
 Shale 
 
 Sandy fireclay... 
 Coaly seam 
 Sandstone 
 Laminated fireclay 
 Coaly shale 
 Fireclay 
 
 Coaly seam 
 Fireclay 
 
 Coaly seam 
 Fireclay 
 
 Coaly seam 
 Fireclay 
 
 Coaly seam ‘ 
 Fine paciseee 
 Coaly seam 
 
 e 
 NONWArFPWWONTWIKBNWNOET 
 
 i 
 
 G10 OS C.0 Ss 20.0.0 O0O.C BC oor 
 nr 
 
 : 6 
 
 The coaly seams of the above section are composed of black carbonaceous mud, 
 with streaks and films of coal. A waterworn sample of coal from the bed of the creek 
 had a specific gravity of 1°57, and contained— 
 
 
 
 Water... a3 ee ee boii a ee OL, 
 Volatile Wy drocscte re "tr os Fe, sas ae le OL 
 Fixed carbon (hard pei coke) sc ube vee ce ROU -OL 
 Ash (white) ... ‘ sas coe pa te eo Ok 
 
 10000 
 
 The strata are horizontal, but about a quarter of a mile down the creek some 
 beds of greenish-grey sandstone, containing silicified wood, and bearing a strong 
 resemblance to the strata of the Upper Series on the Bowen River Coal Field, as exposed 
 in Jack’s Creek, dip slightly to the west. 
 
 In the bed of Walker’s Creek, about two miles above its junction with Reedy or 
 Carborough Creek, three small shafts have been sunk on a coal-seam, but in no case has 
 the bottom of the seam been reached. The following section is seen on the bank and 
 in the shafts. The strata dip at 5° to E.S.E. 
 
168 
 
 Ft. in. 
 Sandy shale with lines of very large ferrugino-calcareous nodules in 
 upper part and lines of ironstone nodules in lower part. (Glos- 
 sopteris abundant; also a specimen of Pecopteris?)*  ... pete a tS Be 
 Laminated fireclay (sometimes sandy) = a os aban 
 Compact fireclay (Ph egbe sie acet he aa a Fe Ube fe) 
 Dark shale... ; a : ap n ae 0 2 
 “a {.Coal 2; oe Tr: a a ore Pa ie ae a aby 4) 
 By : Grey shale ... Say i wn A a be es LP 0to0 13 
 3 s 4 Coal ... é a a des se oak ii ies tee anes 
 F,% | Hard red irou. stone Ay) eee tea ree ap ae he 0to0 8 
 si Coal (bottom not seen) a oi i i oe is Pg he) 
 
 Some sandstone beds in the neighbourhood contain silicified logs, and similar logs, 
 evidently weathered out of the sandstone, bestrew the surface in the neighbourhood so 
 thickly that one might imagine a forest to have been felled on the spot and subsequently 
 petrified. In travelling from the mine to South Fort Cooper I found the country 
 similarly strewn with silicified wood as far as Bee Creek. There can be no doubt that 
 the coal-measures of this district are on the horizon of the Upper Bowen River Forma- 
 tion. A gratifying and promising circumstance is the absence of intrusive igneous rocks 
 from this district. A specimen analysed had a specific gravity of 1°38, and contained — 
 
 
 
 Water... Sn wale “8 sat au ee oo 
 Volatile erdroeaenete Sa 50S Be or Aye eee Oe 
 Fixed carbon (firm hard cokers ae ane ace vee 84°74 
 Ash (pale brown) : oft ra ae ne is) © BO 
 
 10000 
 
 The coal of Walker’s Creek is an anthracite containing a higher percentage of 
 fixed carbon and a lower percentage of earthy impurities than any coal of its class 
 known in Queensland or New South Wales. It approaches in composition some of the 
 best anthracites of Wales and Pennsylvania. The Bee Creek coal visibly contains a 
 large proportion of argillaceous impurity, resulting in 23°61 per cent. of ash. 
 
 In 1889, Mr. A. Gibb Maitland mapped + the Coal-Measures in the neighbourhood 
 of Mackay, and connected his lines with those on the Bowen River, mapped by me in 
 1878. With the Annual Report of the Geological Survey for 1889 a Geological Map is 
 given, showing the connection of the Bowen River Coal Field with that on the head of 
 the Isaacs. 
 
 It appears that the Upper Formation extends south-eastward from the Bowen 
 River up Rosella Creek and the heads of the Bowen, where it is capped by the Desert 
 Sandstone Tablelands known as Mount Leslie and the Redcliffe Range, across the high 
 land dividing the heads of the Bowen, the Suttor, and the Isaacs Rivers and Walker’s 
 Creek, gradually widening from north-west to south-east, and capped at the heads of the 
 Isaacs by the Desert Sandstone Tablelands known as the Carborough Ranges. The 
 Middle Formation has been traced on the north-eastern side of the Upper Formation, 
 beneath which it emerges, from the head of the Bowen River south-eastward to Nebo. 
 The bedded porphyrites emerge from beneath the Middle Formation from the Bowen 
 River to Exmoor Station. The fault already mentioned divides the bedded porphyrites 
 from the metamorphic rocks of the Clarke Range along a line extending from the head 
 
 
 
 
 
 * Probably two species of Glossopteris occur here, one possessing a broad thick midrib. The specimen 
 named Pecopteris? is certainly this genus or a very closely allied one. These plants still remain to be 
 worked out. (R.Z. Junr.) 
 
 + On the Geological Features and Mineral Resources of the Mackay District. Brisbane: by 
 
 Authority ; 1889, 
 

 
 ' 
 % 
 5 
 
 ee 
 
 a 
 
 — 
 
 169 
 
 of Pelican Creek to the Bowen River, near Exmoor. From Exmoor south-eastward to 
 a point between Mount Ilialong and Eungella Station, the fault divides the Middle 
 Formation from the metamorphic rocks. Thence south-eastward to the granite range of 
 Mount Dalrymple the Lower Formation comes in immediate contact with the meta- 
 morphic rocks, sweeps round the granite range, on the coastward side, by Mackay and 
 Bloomsbury Station, and, on the south, surrounds the granite mass of Mount Bridgman 
 and Mount Spencer, reaching the sea near Cape Palmerston. 
 
 Beneath the Desert Sandstone of the Carborough Range the Upper Formation 
 of the Bowen River Coal Field is seen. Plant-remains, including Glossopteris and 
 (7) Sphenopteris, were observed by Mr. Maitland in some sandy micaceous shales at a 
 waterfall in Bee Creek. A few yards up the creek a seam of impure coal, one foot in 
 thickness, dips to N. at 10°. A tributary of the same creek exposes a seam of coal 
 at least six feet in thickness, but interrupted by bands of carbonaceous shale. 
 
 About three miles west of Lenten Downs Station a bed of coal, two feet in 
 thickness and of fair quality, was met with in a well at a depth of about fifty feet. A 
 similar seam was met with in a well between Lenten Downs and Greendale.* 
 
 From the heads of the Isaacs to the heads of the Dawson the whole country 
 appears to be made up of strata belonging to the Bowen River Formation, but our 
 knowledge of this district is very limited. Mr. Daintree, in 1872,+ besides the Bowen 
 River, mentioned the occurrence of Palwozoie Coal-Measures on the Dawson, Comet, 
 Mackenzie, and Isaacs, remarking that “numerous outcrops of coal have been observed 
 on these streams. No commercial use, however, has yet been made of any of them, as 
 the measures generally are too far inland to be made available until the railway system 
 of the country is extended in that direction.” From considerations already given I have 
 divided this area between the Middle and Upper Formations of the Bowen Coal Field. 
 
 Mr. Daintree described, in 1870,f certain auriferous drifts at Cement Hill, about 
 sixteen miles from Clermont. Mr. Rands gave a fuller account of the same deposit in 
 his ‘‘ Report on the Clermont District.” § The hill consists of (1st) fifteen to thirty feet of 
 conglomerate, composed of boulders and pebbles of schist and also small quartz pebbles, 
 the whole cemented together by clayey cement formed from the degradation of the 
 schist. The lower four or five feet of the conglomerate form the washdirt in which the gold 
 is found. (2nd). Beneath the conglomerate isa fine-grained silt or shale, from one to four 
 feet in thickness, dipping W.S8.W. at from 5 to 25°. Numerous well-preserved im- 
 pressions of Glossopteris occur in this silt. (8rd) Beneath the silt or shale is another 
 drift, much finer than the upper one, consisting of small schistose pebbles, but contain- 
 ing much more quartz, the quartz pebbles often predominating. This drift, which is 
 locally known as ‘‘tish,’’. is in places forty feet in thickness. In some parts of the hill 
 the Glossopteris shale rests immediately on the schists, but oftener on the “tish.”’ It is 
 in some places over forty feet in thickness. No gold has been found in the lower drift. 
 
 At Hurley’s, and at the Four-mile near Clermont, the drift is of the same 
 character as that at Cement Hill, and Glossopteris is also found at Hurley’s. 
 
 The Victoria Lead, east of Cement Hill, shows the following section :— 
 
 Feet. 
 Basalt ... = ial =r Ls she vin net ie ozs 40 
 Gravelly quartz drift (lower 3 or 4 feet containing gold) ee p20 60 
 “Tish” as above described ... sa ee oe oye WY we 79 
 
 
 
 * Geol. Obs. at the Heads of the Isaacs, the Suttor, and the Bowen Rivers. By A. Gibb Maitland. 
 Brisbane: by Authority: 1889. 
 
 + Quart. Journ. Geol. Soc. Lond., xxviii., p. 285, 
 
 + General Report upon the Northern District. Brisbane: by Authority; 1870, p. 3. 
 
 § Brisbane: by Authority ;: 1886. 
 
170 
 
 While the presence of Glossopteris was relied upon as an infallible indication that 
 the beds in which it occurred were of Paleozoic age, the above, of course, were ranked as 
 the oldest known auriferous drifts in Queensland, and were supposed to have derived 
 their gold from the denudation of a land surface which existed in Permo-Carboniferous 
 times. Mr. Rands’ recent discovery of Glossopteris in the Upper Cretaceous Desert 
 Sandstone gives, however, a new signification to the argument derived from the presence 
 of that plant. The beds in which it oceurs—at least when it is unaccompanied by other 
 fossils—may be of any age from the Lower Bowen to the Desert Sandstone. 
 
 The same remarks apply to certain deposits in New South Wales, described 
 as quoted below by the late Mr. C. 8. Wilkinson, Government Geologist,* as their 
 supposed Carboniferous age depends solely on the presence of Glossopteris. 
 
 “North of Gulgong, at Tallawang, the coal measures cover a large extent of 
 country, their lowest beds having been found to be payably auriferous. TI reported this 
 interesting discovery to you in November last, stating that during my examination of 
 the Tallawang Gold Field Reserve I observed the important fact that the gold found in 
 the Tertiary alluvial deposits at the old Tallawang and Clough’s Gully Diggings has 
 been chiefly derived from conglomerates in the coal measures. These conglomerates 
 are associated with beds of sandstone and shale, containing Glossopteris, the fossil-plant 
 characteristic of our coal measures. At Clough’s Gully the conglomerate is being 
 worked dn situ, and yields from 1 to 15 dwt. of gold per ton, while nuggets weighing 
 5 oz. have been obtained from it. Several hundreds of tons of the conglomerate (locally 
 termed cement) have been crushed, but as the yield is said to have been patchy or 
 variable, work has been stopped, and the ground is now held under lease. There are, 
 however, a few miners still at work in the adjacent claims, and I took the opportunity 
 of purchasing from one of them a sample weighing 1 oz., of the gold which he was 
 crushing by hand out of hard cement. The gold is coarse in size, remarkably scaly, and 
 waterworn. I hope to secure for the Museum of Mines some samples of the con- 
 glomerate containing gold. Mr. R. McKay, of Clough’s Gully, gave me one small 
 piece showing coarse gold. 
 
 ‘This is the first time that gold has been noticed as occurring in payable quantity 
 in the coal measures of this colony, and it is not unworthy of remark that we here 
 possess one of the most ancient auriferous alluvial deposits in the world!” 
 
 At Blair Athole Station, ten miles north-west of Clermont, in a well sixty feet 
 deep, a seam of coal, together with yellow and grey sandstones, with bands of fine- 
 grained fissile sandstone and shale, were met with, dipping at 10° to S.E. - From the Peak 
 Downs Telegram of 1st March, 1873, we learn that the seam was about six feet thick, 
 and at a depth of about seventy feet from the surface, and that another seam, two feet 
 thick, lay about three feet below it. In a bore sunk by the Peak Downs Copper 
 Company, a hundred yards from the Blair Athole well, a four-feet seam of coal was met 
 with at one hundred feet. 
 
 From the Peak Downs Telegram of 30th November, 1889, we learn that in 1889 
 another shaft was sunk seven hundred yards distant from the well, in which was the 
 following section :— 
 
 Teet. 
 Surface ... AC See eee Be es Hie} ener ieee 
 Sandstone ae a ae ae war ARG ano ane aaitel§) 
 Shale aa ok an em oe Le te re an ets, 
 Sandstone ne sat a oe Se sii Bas £5 tiaee 
 Coal eh ne ie air ant a ere es At 5 
 
 
 
 * Ann. Report Dep. Mines, N. 8, Wales, for 1876 (1877), pp. 173, 174. 
 
171 
 
 The coal was tested by the Locomotive Foreman on the Central Railway. With 
 a consumption of 3 tons 16 ewt., or about 29 lb. per mile, the engine ran 286 miles, 
 with an average load behind the tender of 108 tons. The coal is described as “light,” 
 and its steaming qualities as ‘‘ good.” 
 
 From Dinner Creek, near Stanwell, Mr. James Smith has forwarded to me 
 numerous specimens of Glossopéeris, &c.,* which appear to indicate that in this locality 
 strata equivalent to the Uppér Series occur. Seams of coal have been met with in this 
 neighbourhood. The unaltered, and not much disturbed sandstones and shales of 
 this formation are clearly distinct from the highly inclined, and considerably altered, 
 fossiliferous rocks (Gympie Beds) of Stony Creek, Stanwell, and also from the 
 Mesozoic Beds of Stewart’s Creek, Stanwell. 
 
 From its organic remains, lithological character, and position, I have no hesita- 
 tion in regarding the Upper Bowen Formation as the equivalent of the “ Tomago, 
 East Maitland, Series (productive coal measures), 5,700 feet thick; Dempsey Series 
 (barren freshwater beds), 2,000 feet thick; and Newcastle Series (productive coal 
 measures), about 1,150 feet thick,’ of New South Wales.+ 
 
 
 
 * There are apparently three distinct species of Glossopteris and a Pecopteris. This material has still 
 to be worked out. (R.E. Junr.) 
 
 +A Correlation of the Coal Fields of New South Wales, by T. W. Edgeworth David, B.A., F.G.S. 
 Proc. Austr. Assoc. Adv. Science, 1890, i1., p. 464. 
 
 J. 
 
CHAPTER XIX. 
 THE PERMO.CARBONIFEROUS SYSTEM—continued. 
 
 THE UPPER BOWEN FORMATION OUTSIDE OF THE TYPE DISTRICT—continued. 
 TncLtupINnG TowNsvVILIE, OaAKY CREEK, AND LITTLE RiveR, Cooktown. 
 
 Nortu of the Bowen River, strata of the age of the Upper Formation of the Bowen 
 River Coal Field are met with in the neighbourhood of Townsville and Cooktown. 
 
 A cutting on the Northern Railway, near Stewart’s Creek Station, exposes some 
 thin beds of conglomerates, sandstones, shales, and fireclays, which have yielded Glossop- 
 teris. A sheet of porphyry is intruded aniong the strata. During the progress of 
 some excavations for the purpose of straightening a curve, some thin lenticular seams 
 of coal were exposed. Of one of these I made the following analysis in 1887 :— 
 
 
 
 Water cae. Aeon es eae wet we Saf me eS 
 Volatile hydrocarbons ... sme eat i oe w. 46°66 
 Fixed carbon... ee oa cos ate ee te) OL OO 
 Ash so Ae ee Ac nt Rie 5c Oras 
 
 100°00 
 
 Similar beds are seen on the adjacent Aboriginal Reserve, where an adit driven 
 horizontally into a hillside exposed beds containing Glossopteris and other undetermined 
 plants in large numbers. Here the shales and sandstones are interstratified with beds 
 of volcanic origin. 
 
 At a point on the hillside nearly due south of an old bore sunk by the Townley 
 Coal Company, a sandstone bed, seven inches thick, rests upon shales and is covered by a 
 sheet of lava. Near the south-eastern extremity of the hills, about 180 feet above the sea- - 
 level, blue-black shales and six inches of impure coal lie horizontally beneath volcanic ash. 
 
 At one spot the shales are “ porcellanised,” but the induration does not appear 
 to extend for any great distance. These baked shales dip at 23° to 8.S.E., and rest 
 upon and are covered by volcanic rocks. 
 
 “The age of these volcanic rocks appears to be contemporaneous with the beds 
 at Stewart’s Creek.” * 
 
 At Stewart’s Creek Railway Station the rocks already described are faulted 
 against volcanic ashes. These, at a height of 120 feet above the station, on the western 
 bank of one of the heads of Stewart’s Creek, show what appear to be bedding-planes 
 running north-north-east. Some distance further west, on the fall of the next gully, the 
 ashes are seen to assume a very coarse character, with fragments about the size of an 
 egg. Traced further north, these beds pass almost insensibly into what appears to be 
 a medium-grained granite, the weathered surface of which is often pebbly, suggesting 
 the probability of the granite being metamorphic. Near the summit of the ridge west 
 of the Railway Station, the ashes contain lenticular lava-beds, the internal portions of 
 which are wavy and contorted, looking very like fluxion-structure, but simulating the 
 appearance put on by some rocks which have been subjected to intense pressure. 
 
 * Report on the Physical Geology of Magnetic Island, &, By A. Gibb Maitland. Brisbane: 
 by Authority : 1892, 
 
-_— 
 
 173 
 
 Similar volcanic ashes and lava-beds extend from Stewart’s Creek to Alligator Creek, 
 and form Mount Louisa, Cape Pallarenda on the western extremity, and Cape Cleveland 
 on the eastern extremity of Cleveland Bay, as well as the western corner of Magnetic Island. 
 
 The great thickness of alluvium which covers the stratified rocks north of the 
 Aboriginal Reserve has hitherto formed an insuperable difficulty in the way of ascer- 
 taining whether workable coal-seams exist in the neighbourhood of Townsville. The 
 site of the Caledonia Company’s Bore is only about thirty-five feet above the sea-level, 
 but the alluvium has been ascertained by numerous shallow bores in the vicinity to be 
 from eighty to one hundred and ten feet in thickness. 
 
 A bore recently sunk by the Caledonia Coal Company, about half-a-mile south of 
 the adit above referred to, gives the following section :— 
 
 Ft. in 
 
 Surface Mee ee ~ fe ae te “nf ae pce ts, 
 Sand and stones (water-bed) ae = ae wae tse ecu 
 Gravel and boulders... ies oe Sy: = bie = we Leo 
 Porphyry A 
 Rough grey sandstone 8 
 Rough sandstone 6 
 Dark-brown sandstone 6 
 Coal ee 0 
 Sandstone and ahaloee 2 
 Dark rock 5 
 Blue post (or lava) 17 
 Sandstone : 5 
 Sandy shale with thin vein “of coal 2 
 Conglomerate ‘ 17 
 Sandstone 
 
 Sandstone with vein ‘at ae 
 Shales and sandstone 
 Conglomerate 
 
 Sandstone and shales 
 
 Shale with coal-veins 
 Sandstone and shale 
 Conglomerate 
 
 Fine conglomerate 
 
 Blue post (or lava) 
 Sandstone 
 
 Coal 
 
 Sandstone 
 
 Shales and pamittone Sati ih band of on 
 Shale ... 
 
 Sandstone 
 
 Shale with thin band of Be 
 Sandstone 
 
 Shale ... 
 
 Conglomerate _ 
 
 Blue post (or lava) 
 
 Sandy shale ... os 
 
 Blue post (or lava) ... 
 Sandstone 
 
 Sandy shale ... ee 
 
 Blue post (or lava) ... 
 Sandstone (brown, mipageous) 
 
 pad 
 
 e 
 rt COO OSes 09 Oreo COS OCs Cr Ore OO Co Cr 
 
 _ 
 
 Eee ete Caen gen ome eieeostt ots ees ne 
 
 IDmDNWADAOANODAOSTASO 
 
 vo 
 I 
 wo 
 oO 
 
174 
 
 Similar rocks were met with to about 350 feet, when hard quartzites and fine 
 hard grits were met with, divided by bedding-planes forming an angle of about 45° to 
 the perpendicular course of the bore. Apparently the base of the Coal-Measures had 
 been reached, and an older formation, upon which they lie unconformably, entered upon. 
 
 In the neighbourhood of Cooktown a series of strata, presumably of the age of 
 the Upper Bowen Formation, extends from the right bank of Oaky Creek, two miles 
 above “ Daddy’s Camp,” southward to the tributaries of Deep Creek, between the 
 Byerstown Road and The Bluff—a distance of about six miles—with an average breadth 
 of a mile and a-half. In this area of nine square miles a very considerable thickness of 
 strata must be represented, as they generally dip at high angles. Sections on Oaky 
 Creek show the base of this formation to rest unconformably on the older slates and 
 quartzites, and at the south-east end of The Bluff the conglomerate and sandstones of 
 the Normanby Range (Desert Sandstone) lie on the upturned edges of the strata of 
 the coal-bearing Pane. The strata consist for the most part of greenish-grey 
 sandstones, nha blue shales, and fireclays. 
 
 Between Oaky Creek and the Normanby Range, to the west, I found, in 1879, 
 in Yam Creek and Coal Creek, numerous seams of coal, some of very good quality, but 
 the thickest (¢n Coal Creek, twenty-five miles from Cooktown) was only eight inches. 
 
 A shaft was sunk on the eight-inch seam of coal, in 1879, by the Cooktown 
 Railway League. The shaft went through the bottom of the coal to a total depth 
 of nineteen feet. A drive six feet nine inches long was then made to the dip (88°), 
 when the bottom of the coal was again cut. The seam was then followed down on the 
 dip for fourteen feet six inches. At the north end of the vertical shaft the section 
 was as follows :— 
 
 In. Ft. in. 
 Black shales, with Glossopteris ... cae 17 2 
 
 First coal (good), 9 inches at upper side, 14 inches at lower 
 side of shaft, with a parting of dark shale 23 inches thick 
 at lower side, thinning out to }-inch at re side 
 
 Dark shale ; 
 
 Second coal, impure, Shee brittle, and short, lights in veolour. 
 Fragments of anthracite can be picked from it 
 
 Dark shale a 
 
 Third coal, brittle anthracite 
 
 Grey sandy shales ... 
 
 Hard grey sandstone 
 
 Sandy shale... : 
 
 Hard grey sandstone 
 
 Or bo 
 tolH 
 
 oe 
 
 to 
 to 
 to 
 
 aa 
 
 Nir 
 Oi) OC was Oo OS 
 OO Od NT Or Ot bo 
 wie 
 
 wie 
 
 At the south end of the vertical shaft the section is as follows :— 
 
 In. Ft. in 
 Black shale sf An a3 ee ome oe 
 First {cisy good... at ane ms aoe an a con Soe tO) OSES 
 Coal ) Clay ... ue a ae er ape ef cu one 00 ame 
 Coal, good ... fa v0 ae ara ne we on D5 DOM eg 
 Dark shale ... . : Pe 0 75 
 Second coal, aia 2 >to | OTe 
 Dark shale ... er Aa 33 to O 6 
 Third coal, brittle, Seated inpare . Geto eeOmey) 
 Dark sandy shale Ze7, 
 Sandstone... 0 6 
 Dark sandy shale 0 10 
 
 Sandstone (bottom of shaft) 
 
175 
 
 At the bottom of the underlie shaft the section is as follows :— 
 
 Tn. Tt. in, 
 
 . Coal, good ‘be oh eee en a7 aa . es 
 an {Black shale ... oe. ~ i = Ke ea ea neealo 202 
 Coal, good... oes ee ey, 3 fe ant rae eto. OG 
 
 Black shale ... ; _ 4¢ to 0 8 
 
 Second and third Boats brite: aathese HG) 12 hes hick ee 
 end of shaft, although interrupted by 8 inches of shale 
 2 feet from end er : as be ie! 
 
 From the Oaky Creek beds my ‘Colleague ie Picante among my collection 
 Glossopteris linearis, McCoy, and Glossopteris ampla, Dana. Silicified wood, very much 
 resembling that from the Upper Bowen Formation, is also common. 
 
 The Little River Coal Field, near Palmerville, occurs in a somewhat peculiar 
 position, having been wedged, by two faults, into the midst of an older series of grey- 
 wackes, slates, quartzites, &c. After having been subjected to such a degree of lateral 
 compression that its strata were inclined at high angles, it was covered over by a cake 
 of Desert Sandstone. This cake was subsequently cut through by the Little River (a 
 tributary of the Kennedy), exposing the Coal-Measures and older stratified rocks. 
 
 The coal-bearing strata consist mainly of blue and dark shales, gritty sandstones, 
 and fireclays. The coal-seams are numerous and thick. One is twenty feet in thickness, 
 another eighteen feet, two are eight feet each, two are six feet each, and four are three 
 feet each; but all of these thick seams are of poor quality. They appear to have been, 
 from the first, much mixed with muddy sediment, and to have had much of their volatile 
 matter driven off by the pressure which resulted in the uptilting of the beds. 
 
 An eight-feet seam on the bank of the Little River, near Bower-bird Gully, was 
 analysed by the late Mr. Karl Staiger as follows :— 
 
 
 
 Moisture, with alittle gas... we ae aes .. 18°32 
 Carbon ... si aa ane S60 as ae ... 66°94 
 Ash ae ie a ova Pe oe sr we 15°74 
 
 10000 
 
 I analysed samples from an eight-feet seam on Dave Creek, with the following 
 result :— 
 
 
 
 Water ... con - ses ie oes sie eetOL LO 
 Volatile Hydrocarbons... ae ies eng ee wo. 9388 
 Fixed carbon one 300 vee Gea ... 58°606 
 ASE “ss. at re LE sat ie i .. 31087 
 
 100-00 
 
 Specific gravity, 1°37. 
 Near the junction of the Little River with the St. George River the following 
 section is seen :— 
 
 Ft. in. 
 Coal, good... re ie a ; aS OO 7 
 Dark-grey shales 0 6 
 Coal, good Ore 
 Dark shales ie 0 
 Decomposed carbonaceous Feder 0 3 
 Coal, fair 0 7 
 Grey shales ... x 0 4 
 Dark gnarled shales oe 0 3 
 Grey shales and sandstones, with a few. bands of oolitic ironstone 
 (1 to 2 inches), and impressions of fossil trees __... a4 eee; 0 
 
176 
 
 This coal, on analysis, gave much better results than any of the thicker seams ; 
 in fact, it is one which, if of workable thickness, would take a high place among coals 
 used for steam and smelting purposes. The following is the analysis :— 
 
 
 
 Water ... a oe cae ses eo et) eee 
 Volatile hydrocarbons... ee s ts te ye ay 
 Fixed carbon... ae Sh akc a i ... 62:998 
 Ash 56 5c mae 50 aD sod er .. 8'042 
 
 100-00 
 
 Specific gravity, 1°32. 
 
 The only fossil from the Little. River determined by my Colleague is Glossopteris 
 Browniana, Brong. 
 
 If the evidence for the Paleozoic age of the Oaky Creek and Little River 
 deposits rested solely on the presence of Glossopteris, it would be of little value, seeing 
 that Glossopteris has been detected in beds as new as the Desert Sandstone ; but in the 
 cases before us, the coal-bearing beds are not only upturned, but are covered uncon- 
 formably by the Desert Sandstone itself. 
 
 In “ Notes on the Geology of Hann’s Exploring Expedition,”* with which Mr. 
 Norman Taylor has obligingly furnished me, the following passages occur :—“ At Camp 
 16, on the Mitchell River (Camp 78 on the return journey), I found in the river-bed 
 fragments and blocks of coal shales, with thin seams of bright coal, and on searching 
 carefully I discovered pieces of a whitish indurated shale, containing indistinct plant- 
 remains and an undoubted fragment of Glossopteris. (The shales are identical with 
 some in the Blue Mountains of New South Wales, north of Wallerawang, and again 
 at Tallawang, north of Gulgong.)” . . . . “About a mile south of this camp is a 
 low table-topped rise, consisting of horizuntal white and grey shales and a cherty- 
 looking rock, with fragments and stems of plants and traces of Glossopteris in situ. 
 This rests on porphyry, which forms a series of rocky hills two miles further south, 
 extending seven miles south-easterly to the foot of and overlooking some high table- 
 topped Carboniferous ranges (composed of sandstones, grits, and conglomerates, with 
 silicified wood) in that direction.” 
 
 The occurrence of Glossopteris alluded to by Mr. Taylor has always been a 
 puzzle to me. It would appear as if the plant had been found in the horizontal sand- 
 stones and shales, which I have always regarded as of Desert Sandstone age, and on this 
 evidence, in my “ Handbook of Queensland Geology’’ (1886), and “ Geological Map of 
 Queensland ’’ (1886), I classed the Mount Mulligan Tableland as a continuation of Mr. 
 Taylor’s “ Carboniferous Range,” I confess with considerable reluctance. Since then, 
 however, Mr. Rands’ discovery of Glossopteris in a portion of the Desert Sandstone, 
 which clearly overlies unconformably the Lower Cretaceous Rolling Downs Formation, 
 removes any difficulty there may have been in regarding Mr. Taylor’s Glossopteris- 
 bearing beds as of Desert Sandstone age, and I have restored them accordingly to that 
 formation in the Geological Map issued herewith. 
 
 J. 
 
 *For a full account of the late Mr. W. Hann’s Exploring Expedition in Northern Queensland (to 
 which Mr. Norman Taylor was attached as Geologist), see Proc. R. Geogr. Soc., 1874, xviii., pp. 87-107. 
 
CHAPTER XxX. 
 
 THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 LIFE OF THE UPPER BOWEN FORMATION. 
 
 Tue fossils occurring in the Upper Bowen River Formation are :—Phyllotheca australis, 
 Brong., Sphenopteris lobifolia, Morris, 8. flewuosa, McCoy, 8. crebra, Ten. Woods, 
 Glossopteris Browniana, Brong., G. linearis, McCoy, Coniferous wood, Derbyia senilis, 
 Phill., Productus brachytherus, G. Sby., and Goniatites, sp. ind., Pl. 15, fig. 5. 
 
 Of these, Phyllotheca australis, Sphenopteris flexuosa, and S. crebra, are peculiar 
 to this formation. 
 
 Productus brachytherus occurs not only in this formation but also in the Gympie 
 and Middle Bowen Formations. 
 
 Sphenopteris lobifolia, Glossopteris Browniana, G. linearis, and Derbyia senilis, 
 occur in both the Middle and Upper Bowen Formations. 
 
 Goniatites, sp. ind., Pl. 15, fig. 5, occurs in both the Upper Bowen and the 
 Gympie Formations. 
 
 The following Genera are common to the Upper Bowen and Gympie Forma- 
 tions :—Mo.uvsca: Productus and Goniatites. 
 
 There are not even any. genera common to the Upper Bowen and Star 
 Formations. 
 
 The following Genera are common to the Upper and Middle Bowen Formations :— 
 Pianta: Sphenopteris and Glossopteris. Moutusca: Derbyia, Productus,and Goniatites. 
 
 J. 
 
CHAPTER XXI. 
 
 LIST OF THE FOSSILS OF THE PERMO-CARBONIFEROUS SYSTEM, 
 
 SHowrna THEIR Horizons. 
 
 Noves. 
 
 The Gympie Series (Column I.) includes, besides the Gympie area (G.), the following :—‘‘ Rockhampton 
 District ” (R.), Lake’s Creek and Training Wall Quarries (L.), Kooingal (K.), Stanwell, in part (8.), 
 Encrinite Creek (E.), Fenestella Hill (F.), Athelstane Range (A.), Don River (D.), Crow’s Nest (C.), 
 Blackfellow’s Diggings (B.), Lilymere (LM.), Kariboe Creek, Cania (KC.), Yatton (Y.), Yarrol Lime- 
 stone (YL.), Hodgkinson Gold Field (H.), Raglan* (RL.), Beaconsfield (BF.), Langmorn (LR.), 
 Broadsound Ranges (BR.), Apis Creek (AC.) 
 
 The Star Beds(Column IT.) include, besides the Star area (S.), the following :—Keelbottom (K.), Drummond 
 (D.), Mount Wyatt (W.), Canoona (C.), Broken River (B.) 
 
 The Middle or Marine Series (Column III.) includes, besides the Middle Series as developed on the Bowen 
 River (MB.), the following :—Cracow Creek, in part (C.), Dawson River, in part (D.), Mount Britton 
 (B.), Stanwell, in part (8.), Banana Creek (BC.), Springsure (SS.) 
 
 The Upper or Freshwater Series (Column IV.) includes, besides the Upper Series as developed on the Bowen 
 River (UB.), the following :—Cracow Creek, in part (C.), Dawson River, in part (D.), Little River, 
 Cooktown (L.), Oakey Creek, Cooktown (O.), Stewart’s Creek, Townsville (S.), Walker’s Creek, Nebo 
 (W.), and Dinner Creek, Stanwell (DC.) 
 
 
 
 Il. IV. 
 L | Middle Upper or 
 Systematic Position and Name. Gympie | Aeeenee pee uk pertaen 
 Series. | Bowen River | Bowen River 
 | Coal Fiel@, | Coal Field. 
 
 
 
 Kingdom—PnrantTm. 
 Section— CRYPTOGAMI®. 
 Class—ACOTYLEDONES. 
 Order—CALAMARI®. 
 Family—EQUISETACER. 
 Genus—CaLAMITEs. 
 Calamites varians, Germar. nas “00 es ae ane D 
 sp. ind. ae se one toe L 
 
 ” ” 
 
 Genus—ASTEROCALAMITES. | 
 
 Asterocalamites scrobiculatus, Schloth., Pl. 4, figs. 11, 12 at D 
 
 
 
 Family—ScHIzoNnEURID®. 
 Genus—PHYLLOTHECA. 
 Phyllotheca australis, Brong. ... oh ars Ana wae 455 ret UB 
 
 
 
 Order—FInLices. | 
 Family—SPaENOPTERIDE®. 
 Genus—SPHENOPTERiS. 
 Sphenopteris lobifolia, Morris... sis eet 460 ee C, 2. MB 
 flexuosa, McCoy ... Rel sins 500 Sige pn ses 
 crebra, Ten. Woods... ue ae aes mes es aie 
 
 q 
 Bug 
 
 Family—PaLm®OPrERIDE®. 
 Genus—ANEIMITES. 
 Aneimites austrina, Eth. fil. ae see Sor a by, D 
 
 
 
 
 
 
 
 
 
 * T regard this as Devonian. See Footnote, p. 89. (R.E. Junr.) 
 
179 
 
 LIST OF FOSSILS OF THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 On ne ee 
 
 Systematic Position and Name. 
 
 Family— DicrroTmNIoPTERIDE®. 
 Genus—GLossoPTERIS. 
 : figs. 9, 10 
 Sy linearis, McCoy 
 “ ampla, Dana? Pl. 16, fig. 7 
 
 Order-—LYCoPODIACE®. 
 Family—LEPIpODENDRID®. 
 Genus—LEPIDODENDRON. 
 
 Lepidodendron australe, McCoy, Pl. 5, figs 1-10 
 e veltheimianum, Sternb. ... 
 . sp. mmd., Pl. 6, figs. 1,'4 ... 
 
 Genus—CYcLosTiGMA. 
 Cyclostigma sie Feist. 
 
 eee eee 
 
 = ., Feist., allied to ic Kiltorkense 
 Genus—STIGMARIA. 
 Stigmaria, sp.ind., Ten. Woods ... wes HAR 
 
 Section—PHANEROGAMIA. 
 Class—DIcoTYLEDONES. 
 Order—CYCADACER. 
 Family—CorDAITER. 
 Genus—CorDAITES. 
 Cordaites australis, McCoy ? 
 
 Order—ConiFERE at 
 
 Kingdom—ANIMALTA. 
 Sub-Kingdom—PrRoT0z0A. 
 Class—SPon@IpDa. 
 Order—MONACTINELLIDE. 
 Family— ? 
 Genus—LASIOCLADIA. 
 
 Lasiocladia? Hindei, Eth. fil., Pl. 41, figs. 1, 2 
 
 Sub-Kingdom—C@LeENTERATA. 
 Class—ACTINOZOA. 
 Order—Rvaosa. 
 Group—ZAPHRENTOIDEA. 
 Family—ZaPHRENTIDR. 
 Genus—ZAPHRENTIS. * 
 
 Zaphrentis profunda, Eth. fil., Pl. 44, fig. 1... 
 
 Group— CyATHOPHYLLOIDEA. 
 Family—CYATHOPHYLLIDR. 
 Genus—CYATHOPHYLLIUM. 
 Cyathophyllum, sp. ind., Pl. 3,f.10  ... 
 : sp. ind, Pl. 7, f. 1 one 
 
 Glossopteris Browniana, Brong., Pl. 16, figs. 6,8; Pl. 
 
 
 
 tit 
 Gympie 
 Series, 
 
 ?G 
 
 BF 
 LR 
 
 | 
 
 
 
 
 
 III. 
 . Middle 
 Tes or Marine 
 Star Beds, Series— 
 Coal Field. 
 2 MB 
 566 MB 
 a, ? MB 
 8, W, C, B, D 
 D 
 8,D 
 D 
 w,c¢ 
 D 
 D 
 MB 
 
 
 
 Tis 
 Upper or 
 Freshwater 
 Series— 
 
 Bowen River | Bowen River 
 
 Coal Field. 
 
 UB, D, 0, I, 
 8, W, DC 
 0, UB 
 
 UB 
 
 
 
 
 
180 
 
 LIST OF FOSSILS OF THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 
 
 Systematic Position and Name. 
 
 
 
 Section—PERFORATA. 
 
 Family—AULOPORIDE. 
 
 Genus—CLADOCHONUS. 
 Cladochonus tenuicollis, McCoy ... 
 
 Order—MonTICULIPORIDEA. 
 
 Family—MonTicuLipoRipz. 
 
 Genus—MonvTicuLivora. 
 Monticulipora, sp. ind., Pl. 38, figs. 1, 2 
 
 Genus—SrEnopora. 
 Stenopora australis, Nich. and Eth. fil., Pl. Bs gee 5-8 
 - Leichhardtii, Nich. and Eth. fil, 6, figs. 
 9, 10; Pl. Clee 
 A Jackii, Nich. and Eth. fils 
 3 Sp. ae Pl. 7, figs. 3-5 
 3 gimpiensis, Eth. ‘fil., io: figs. 14, 15 
 
 Pl. 6, figs. 11-13 
 
 Sub-Kingdom—EcHInopERMATA. 
 Section—PELMATOZOA. 
 Class—CRINOIDEA. 
 Order—CoabDuNaAtTa. 
 Family—ActinocrinIDm. 
 Genus—ACcrINocRINUS, 
 Actinocrinus, sp. ind., Pl. 7, fig. 9 
 
 Family—PuLatyceinipz, 
 Genus—PLATYORINDS. 
 Platycrinus ? nua, Eth. fil., Pl. 88, fig. 8 pat 
 
 Order—InapUnata. 
 Family—Porertocrinipm. 
 Cup of Crinoid, Pl. 44, fig. 7 nas sac 
 Poteriocrinus ? Smithii, Eth. fil., Pl. 8, fig. 1 
 erassus, Miller > Pl, if fig. 6 
 Arms of Crinoid, Pl. 7, ‘fig. 7 
 A ape ed big fig. ee 
 Impressions of Crinoid Caly, Pi. 44, fig. 8 
 Crinoid Stems : 3 
 
 Class—BLAsToIpEA. 
 Order—REGULARES. 
 Family—PrntReMitipm. 
 Genus—Mrsoptastus, 
 
 Mesoblastus? australis, Eth. fil., Pl. 44, fig. 2 
 Family—GRaNATOBLASTID®. 
 Genus—GRANATOCRINUS. 
 
 Granatocrinus? Wachsmuthi, Eth. fil., Pl. 7, fig. 10 
 Family—TRoostoBLAstIp™. 
 Genus—TRIC@®LOCRINUS. 
 
 Tricelocrinus ? Carpenteri, Eth. fil., Pl. 44, fig. 3 
 
 Section—EcuInozoa 
 Class—EcHINOIDEA. 
 Order—PALECHINOIDFA. 
 Family—ARCHHOCIDARID &. 
 Genus—ARCHOOIDARIS. 
 Archeocidaris, sp. ... ee ee 
 
 
 
 
 
 
 
 
 
 III. IV. 
 Middle Upper or 
 as . IL. or Marine | Freshwater 
 Gympie Star Beds. Series— Series— 
 Rertes: Bowen River | Bowen River 
 Coal Field. | Coal] Field. 
 R 
 kK 
 MB 
 MB 
 eee MB 
 K 
 G 
 R 8 
 B 
 R 
 8 
 E, F 
 8s 
 8 
 R 
 K,5,A “ 88 
 R 
 8 
 R 
 R 
 
 
 
181 
 
 LIST OF FOSSILS OF TILE PERMO-CAKBONIFEROUS SYSTEM—continued. 
 
 
 
 Systematic Position and Name. 
 
 Sub-Kingdom—ANNULOSA. 
 Class—CRUSTAOEA. 
 Order— OstTRacopa. 
 Family—LrPERrDITIp2#. 
 Genus— BEYRICHIA. 
 
 Beyrichia varicosa, T. R. Jones, Pl. 7, fig. 15 ... 
 
 Order—TrILopiTa. 
 Family—PR@tip&. 
 Genus— PHILLIPSIA. 
 Phillipsia dubia, Eth., Pl. 7, fig. 12; Pl. 8, figs. 5,6; 
 Pl. 44, fig. 4 
 Woodwardi, Eth. fil, Pl. 7, figs, 11, 18; 
 Pl. 8, fig. 6; Pl. 44, figs. 5, 6 
 Fe ? sp. ind. ses He 5 
 
 Genus—GRIFFITHIDES, 
 Griffithides seminifera, Phill ?, Pl. 7, fig. 14 
 
 Sub-Kingdom— Mo tivsoa. 
 Section— MoLbuscorpEA. 
 Class—Potnyzoa. 
 Order—GYMNOLEMATA, 
 Sub-Order—CrYcLostoMATA. 
 Family—FeEnestEeLLip®, 
 Genus—FENESTELLA. 
 Fenestella fossula, Lonsd., Pl. 9, figs. 4, 5 
 
 internata, Lonsd., Pl. 9, figs. 6, 7 
 
 a sp. ind. .., re bist so vee 
 
 i multiporata, De Kon. Pl. 8, figs. 7, 8 
 
 Genus—POLYPORA. 
 Polypora? Smithii, Eth. fil., Pl. 9, figs. 1-3; ? Pl. 44, 
 figs. 9, 10. 
 
 Genus—PROTORETEPORA. 
 
 Protoretepora ampla, Lonsd. ... ce ey: a 
 5 an var. Woodsi, Eth. fil., Pl. 8, 
 fig. 12 
 
 % ¥ var. Konineki, Eth. fil. 
 Family—THAMNISCIDE. 
 Genus—GLAUCONOME, 
 
 Glauconome, sp. ind., Pl. 44, fig. 11 
 
 Family—PETALOPORID mE. 
 Genus—RHOMBOPORA. 
 Rhombopora? laxa, Uth., Pl. 9, figs. 8, 9 
 
 Family— 
 Genus—MYRIOLITHES. 
 Myriolithes? queenslandensis, Uth. fil. ... 
 
 Class—BRACHIOPODA. 
 Order—TRETENTERATA. 
 Family —TEREBRATULIDE. 
 Genus—DIELASMA. 
 
 Dielasma cymbeformis, Morris, Pl. 9, figs. 10, 11 
 
 Le 
 Gympie 
 Series. 
 
 G, B, L 
 
 G, K 
 
 B, F, G 
 
 B, G, BR, AC 
 
 
 
 LM, RL* 
 
 2G me IV: 
 Middle Upper or 
 or Marine | Freshwater 
 series— Series— 
 
 Bowen River | Bowen River 
 Coal Field. Coal Field. 
 
 
 
 
 
 MB 
 
 MB 
 
 MB 
 
 
 
 
 
 MB 
 
 
 
 
 
 * T regard this as Deyonian. See Footnote, p. 89. 
 
182 
 
 LIST OF FOSSILS OF THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 Systematic Position and Name. 
 
 
 
 
 
 Dielasma sacculus, Martin, var. ... 
 y af var. hastata, ue de C. Sty. 
 rr sp. ind., Pl. 40, figs. 1, 
 
 Family —SPrrtFERID®. 
 Genus—SPIRIFERA. 
 Spirifera striata, Martin? Pl. 9, fig. 16 sre 
 5 sp. ind. (a.), Pl. 9, fig. 12 nde 
 “fs vespertilio, G. B. Sby., Pl. 10, fig. 8. 2 
 ~ convoluta, Phill., Pl. 10, figs. 10, gE e sh 
 i lata, MeCoy ate sac 40 
 Clarkei, De Kon. Pl. 10, fig. 16? 
 trigonalis, Martin, PI. 9, fig. 15 fen “or 
 var, acuta, Eth., Pl. IO), ite PY 
 F A var. crassa, De Kon., Pl. ikl, ie 5 
 ms dubia, Eth., Pl. 10, fig. 14 5c 
 os Sp. ind. (0), Pl. 38, figs. 4-6 ... 
 a tasmaniensis, Morris, ELSLO; oe 1, 215 
 Stokesii, Konig, Pl. 10, figs. 2-4 ace 
 _ pinguis, J. Sby. 6 
 
 » ” 
 
 i brcarinata, th. 41... PL 10, figs. 9, 13; 
 Pl. 37, fig. 17; Pl. 11, figs. 1-3 
 nH Strzeleckii, De Kon., Pl. 10, figs. 5-7 oe 
 
 Genus—SPIRIFERINA. 
 Spiriferina duodecimcostata, Dag Pl. 44, me 12 
 
 ; sp. ind... 
 
 Genus—RETIOULARIA. 
 Reticularia lineata, Martin ? rages 
 pp Urei, Fleming nee FE te 
 
 Genus—MArtTINniA. 
 Martinia? productoides, Eth. fil., Pl. 11, figs. 6-11 
 
 Genus —MARTINIOPSIS. 
 Martiniopsis ? subradiata, G. B. Sby., Pl. 11, fig. 14 ... 
 
 a subradiata, var. Morrisii, Eth. fil, 
 Pl. 11, figs. 12, 13? 
 f Darwiniti, Morris, Pl. 9, figs. 13, 14; 
 
 Pl. 39, figs. 5-7 
 
 Family—NvcLEosPIRID ®. 
 Genus—ReEtTzIA. 
 Retzia radialis, Phill., Pl. 11, figs. 24, 25 “06 50 
 Ay ie lilymerensis, "Eth. fil., Pl, 11, figs. 20-22 
 
 Family—ATHYRID. 
 Genus—ATHYRIS. 
 Athyris Roysii, Leveillé, Pl. 11, fig 15... Gee si 
 »  ambigua, J. de C. Sby. ae 3 
 »  Randsi, Eth. fil., Pl. 11, figs. 16-18 
 
 Family--RHYNCHONELLIDS. 
 Genus— RHYNCHONELLA. 
 Rhynchonella pleurodon, pai Jel ai wifes Bh 
 3 sp. ind, AoC one tee 
 
 
 
 
 
 UF 
 Gympie 
 Series. 
 
 eos 
 Dy - 
 
 File 
 
 LM 
 
 KO 
 KC 
 
 
 
 
 
 TE, 
 Star Beds. 
 
 
 
 
 
 
 
 
 
 LEE. IV. 
 Middle Upper or 
 or Marine Treshwater 
 Series— Series— 
 
 Bowen River | Bowen River 
 Coal Field. Coal Field, 
 
 BC 
 
 MB 
 
 MB 
 MB 
 
 MB, BC 
 BO, B 
 
 ?B 
 
 MB, BO, B 
 
 MB, B 
 
183 
 
 
 
 LIST OF FOSSILS OF THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 EIS LV 
 L Middle Pd ad oe 
 Systematic Position and Name. Gympie yates eee arlene 
 Series. Bowen River | Bowen River 
 Coal Field. | Coal Field. 
 Family—OrrtHID&. 
 Genus—ORr?raHIs. 
 Orthis resupinata, Martin, Pl. 11, figs. 26, 28 8, A, KC 8 
 » australis, McCoy, Pl. 11, figs. 27, 29 8, R 
 Family—STROPHOMENID®. 
 Genus—STROPHOMENA. 
 Strophomena rhomboidalis, vay. analoga, Phill., Pl. 12, G, BR 8 
 figs.8,9; Pl. 40, fig. 6 
 Genus—DrrBytia. 
 Derbyia senilis, Phill. MB 
 Family— Propuctipm. 
 Genus—PropvUctTUsS. 
 Productus cora, D’Orb., Pl. 12, fig. 14; Pl. 13, fig. 1 G, 8, L B 
 Pl. 38, fig. 11 
 . brachytherus, G. Sby., Pl. 12, figs. 10-13; | F, 5, s, Ke, MB, B UB 
 Pills, figs? 3.21. 44, fig. 14 YL 
 % subquadratus, Morris, Pl. 38, figs. 7-10; Pl. a0 BF MB, B 
 40, fig. 5. 
 undatus, Defrance, Pl. 12, fig. 16 8 
 at semireticulatus, Martin ? 8, KO 
 . longispinus, J. Sby.? ... D 
 x sp. ind. (a.), Pl. 18, fig. 6 YL 
 * sp. ind. (6.), Pl. 12, fe. 16 8 
 . sp. ind. (e.), Pl. 18, fig. 4 3 
 " sp. ind. (d.), Pl. 40, fig. 4 R 
 #4 sp. ind. (e.), Pl. 37, fig. 18 es B 
 > sp. ind. (f.), Pl. 44, fig. 13 Y 
 Genus—STROPHALOSIA. 
 Strophalosia geehe, Eth., Pl. 13, figs. 12-17; Pl. 14, MB, 83 
 fig. 19 
 . Gerardi, King, Pl. 18, fig. isin Tee eh, MB, BO 
 fig. 18; Pl. 40, figs. 7, 8 
 Genus—CHONETES. 
 Chonetes cracowensis, Kth., Pl. 13, fig. 9 A 8 © 
 a sp. ind. (a), Pi. 13, fig. 10; PL 3i, figs. 21, 22 AP 8, K 
 73 sp. ind. (b.), Pl. 13, figs. 7, 8, 13 any A, 8 
 3 sp. tnd, (c), 1a B¥f fig. 20 : ie K 
 + sp. ind. (d), Pl. 37, fig. 19 oi . B 
 Order—CLISTENTERATA, 
 Family—Line@vrip2. 
 Genus—LINnGULaA. 
 Lingula mytiloides, J. Sby.? Pl. 13, fig. 19 KC 
 Section—MOottivusca VERA. 
 Class—PELECYPODA. 
 Order—OstTRACEA. 
 Family—PrEctTINIDE. 
 Genus— ENTOLIUM. 
 Entolium, sp. 8 
 Genus—EvcHonpDRIA, 
 Euchondria, sp. ... ae 8 
 
 
 
184 
 
 LIST OF FOSSILS OF THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 
 
 
 
 Systematic Position and Name. 
 
 
 
 Family—AVICULOPECTINIDE. 
 Genus-—AVICULOPECTEN. 
 Aviculopecten subquinquelineatus, McCoy 
 
 limeformis, Morris? Pl. 14, fig. 1 
 
 3 ? imbricatus, Eth. wae 
 _ multiradiatus, Eth. 
 
 rf Laurenti, Eth. fils els 43, ‘figs. 3, “4 
 
 Genus—DELTOPECTEN. 
 Deltopecten illawarrensis, Mor., Pl. 41, fig. 3; Pl. 43, 
 
 fig. 2 
 
 Genus—PTERINOPECTEN. 
 Pterinopecten Devisii, Eth. fil., Pl. 40, fig. 9 
 
 Order—MYTILACEA. 
 
 Family—AVICULIDE. 
 
 Genus—MERISMOPTERIA. 
 Merismopteria macroptera, Mor. 
 
 Family—Myrinipz. ~ 
 
 Genus—MytiILors. 
 Mytilops ? corrugata, Eth. fil., Pl. 40, fig. 11 ... 
 »  ¢ Sp.ind., PJ. 14, fig. 20 mae sae 
 
 Genus—MopIioMoRPHA. 
 Modiomorpha? Daintreei, Eth. fil., Pl. 14, fig.13 ... 
 hy mytiliformis, Eth. fil., Pl. 14, fig. 5; 
 PI. 40, fig. 4 
 
 Order —AROACEA. 
 Family—ARcipZ. 
 Genus—PARALLELODON. 
 Parallelodon costellata, McCoy, Pl. 40, figs. 12, 13 
 
 Family—Nvcvxrip. 
 Genus—Nuoucuta. 
 Nucula, sp. ind., Pl. 40, fig. 10 
 
 Family—NvovuLanips#. 
 Genus—NUcuULANA. 
 Nuculana, sp. ind., Pl. 14, fig. 17... 
 
 Order—LvcINAcEA, 
 Family—SoLemyipz. 
 Genus— SOLEMYA. 
 
 Solemya Edelfelti, Eth. fil., Pl. 14, fig. 16 
 
 Family—AsTaRTID =. 
 Genus—PLEUROPHORUS. 
 Pleurophorus Randsi, Eth. fil., Pl. 14, fig. 14 ... 
 
 Genus—ASTARTELLA. 
 Astartella ?rhomboidea, Eth. fil., Pl. 14, fig. 15 
 
 Genus—CYPRICARDELLA. 
 Cypricardella Jackii, Eth. fil., Pl. 14, figs. 11, 12 
 
 Genus—ASTARTILA. 
 Astartila cytherea, Dana, Pl. 14, figs. 3, 4 
 
 
 
 
 
 Ke 
 Gympie 
 Series. 
 
 ?G, PY 
 
 K,G@ 
 C,B 
 
 KO 
 
 YL 
 
 
 
 II. 
 Star Beds, 
 
 
 
 III. 
 Middle 
 or Marine 
 Series— 
 
 Bowen River 
 
 Coal Field. 
 
 MB 
 MB 
 
 MB 
 
 
 
 
 
 IV. 
 Upper or 
 Freshwater 
 Series — 
 Bowen River 
 Coal Field. 
 
185 
 
 LIST OF FOSSILS OF THE PERMO-CARBONIFEROUS SYSTEM—continued. 
 
 Systematic Position and Name. 
 
 
 
 Order—CHAMACEA. 
 Family— TRIDACNID. 
 Genus—EURYDESMA. 
 Eurydesma cordata, Morris 
 + sacculus, McCoy 
 
 Order—VENERACEA. 
 
 Family—Carpiipz. 
 
 Genus—ConooarDIUM. 
 Conocardium australe, McCoy, Pl. 14, fig. 6 
 
 Order—Myacra. 
 Family—ANATINID. 
 Genus—CHNOMYA. 
 Chenomya ? Etheridgei, De Kon. ae 
 ts 2? carinata, Kth. fil., Pl. 43, igs. 5, 6 
 FF 2? acuta, Eth. ... ‘ 
 a ? bowenensis, Eth. fil. 
 
 Genus—EDMONDIA. 
 Edmondia ? obovata, Eth.... sae es ABS 
 
 Genus —SANGUINOLITES. 
 Sanguinolites concentricus, Eth., Pl. 48, fig. 7 ... 
 
 Family—Sax1cavipH. 
 Genus—PacHYDoMvs. 
 Pachydomus globosus, J. de C. Sby. 
 
 Genus—M moni. 
 Meonia carinata, Mor. 
 » recta, Dana 
 
 Class—GASTEROPODA. 
 Order—PRoOSsOBRANCHIATA. 
 Family—Naricip». 
 Genus—NatTICopsis. 
 Naticopsis? harpeformis, Eth., Pl. 5, fg. 10:; 
 A variata, Phill. ? F a 
 $ sp. ind. oes nee 
 
 Family—PYRaMIDELLIDE. 
 Genus—LoxonEeMa. 
 Loxonema, sp. ade age 
 
 Family—EvoMPHALipz. 
 Genus—EvomMPHALUS. 
 Euomphalus, sp. 
 
 Genus—PLATYSCHISMA. 
 Platyschisma oculus, J. de C. Sby., Pl. 15, figs. 3, 4 
 a rotunda, Eth., Pl. ‘15, fig. 6 
 
 Family—PLEUROTOMARIIDS. 
 Genus—PLEUROTOMARIA. 
 
 Pleurotomaria carinata, J. de C. Sby., Pl. 15, fig. 16... 
 
 Genus—Movrtnonia. 
 Mourlonia Strzeleckiana, Moy., Pl. 15, fig. 2 ... 
 ry ? coniformis, Eth. fil., Pl. 41, fig. 5 
 
 
 
 
 
 III. 
 I Middle 
 ‘pi 10 or Marine 
 oe Star Beds. Series— 
 ‘ Bowen River 
 Coal Field. 
 es . 
 x 
 le 
 PG ae BC 
 BO 
 MB 
 MB 
 qa 
 G 
 . MB 
 . MB 
 MB 
 D 
 8 
 8 
 8 
 8 
 8 
 be c 
 G 
 LM, YU 
 ave eee BC 
 
 
 
 TNE 
 Upper or 
 Treshwater 
 Series— 
 Bowen River 
 Coal Field. 
 
186 
 
 LIST OF FOSSILS OF THE PERMO-CARBONIFEROUS SYSTEM— continued. 
 
 
 
 Systematic Position and Name. 
 
 
 
 Genus—YVANIA. 
 Yvania Konincki, With. fil., Pl. 41, fig. 7 
 
 Genus—LUcIELLA.” 
 Luciella? Graye, Eth. fil., Pl. 41, fig. 6 
 
 Genus—MURCHISONIA. 
 Murchisonia carinata, Eth., Pl. 15, fig. 9 
 
 » sp. (a) 
 ” sp. (b) 
 5 sp. (c) 26 
 
 Family—BELLEROPHONTID®. 
 Genus—BELLEROPHON. 
 
 Bellerophon stanvellensis, Eth. fil., Pl. 15, figs. 11-13 
 Genus—BuvoantIa. 
 
 Bucania textilis, De Kon., Pl. 41, fig. 8 
 
 Genus—PoRcELLIA. 
 Porceilia Pearsi, Eth. fil., Pl. 15, figs. 7, 8 
 
 Class—PTEROPODA. 
 Order—THECOSOMATA. 
 Family—ConvuLaRiip®. 
 Genus—ConvmLaRiA. 
 Conularia tenuistriata, McCoy ... 
 3 sp.tnd., Pl. 41, fig. 10... 
 
 Class—CEPHALOPODA. 
 Order—TrETRABRANCHIATA. 
 Family—NavtTiLipm, 
 Genus— NAUTILUS. 
 Nautilus, sp. 
 is ? ammonitiformis, 
 Pl. 41, fig. 9 
 
 Family—OrTHOOCERATID®. 
 Genus—ORTHOCERAS. 
 Orthoceras, sp. ee ate eh 
 
 Eth. fil, Pl. 39, fig. 9; 
 
 Genus— GY ROCERAS. 
 Gyroceras dubius, Eth. fil., Pl. 41, fig. 12 
 
 Family —GonIAtitiIpm. 
 Genus—GonIATITES. 
 Goniatites micromphalus, Moy. ... ae 
 FS sp. ind., Pl. 15, fig. 5 . 
 m planorbiformis, Eth. fil., PL Al, fig. 9 9 
 y sp. ind., Pl. 15, figs. 14, ‘15 36 
 
 Sub-Kingdom—VERTEBRATA. 
 Class—PIsczs. 
 Order—CHONDROPTERYGII. 
 Family—CocuHiopontTipm. 
 Genus—DELToDUS. 
 
 Deltodus ? australis, Eth. fil., Pl. 39, fig. 11 
 
 Order—GANOIDET. 
 
 Family—PaLmoniscipm. 
 
 Genus—PALZONISOUS. 
 Paleéoniscus Randsi, Eth. fil. 
 
 
 
 
 
 a I 
 Gympie 
 Series. 
 
 BAY 
 
 R 
 
 
 
 INE 
 Star Beds, 
 
 
 
 
 
 IIl. IV. 
 Middle Upper or 
 or Marine | Freshwater 
 Series— Series— 
 Bowen River| Bowen River 
 Coal Field. Coal Field. 
 
 BO 
 BO 
 B 
 MB 
 UB 
 
 
 
187 
 . SYNOPSIS. 
 The Gympie Beds contain— 
 95 species peculiar to themselves. 
 12. ,, in common with the Star Beds, 
 
 iy OP os - ,, Middle Series of the Bowen River Coal Field. 
 ” ” ” Upper » ” » 
 
 The Star Beds contain— 
 19 species peculiar to themselves. 
 12. ,, in common with the Gympie Beds. 
 Sr a 3 rs Middle Series of the Bowen River Coal Field. 
 
 The Middle Series of the Bowen River Coal Field contains— 
 34 species peculiar to itself. 
 17. ,,_ ~+in common with the Gympie Beds. 
 12 5 » Star Beds. 
 Gar, a », Upper Series of the Bowen River Coal Field. 
 
 The Upper Series of the Bowen River Coal Field contains— 
 3 species peculiar to itself. 
 » Imcommon with the Gympie Beds. 
 » » » Middle Series of the Bowen River Coal Field. 
 
 bo 
 
 for) 
 
CHAPTER XXII. 
 
 THE ORGANIC REMAINS OF THE PERMO-CARBONIFEROUS SYSTEM. 
 
 Witn Drscriprions OF THE SPECIES. 
 
 Kingdom—PLANTA. 
 Section—CRYPTOGAMIA. — 
 Class—ACOTYLEDONES. 
 Order—CALAMARIEX. 
 Family—EQUISETACEA. 
 
 Genus—CALAMITES, Suckow, 1784. 
 (Act. Acad. Theodora-Palatina, v., p. 359.) 
 
 CALAMITES VARIANS, Germar. 
 Calamites varians, Germar, Verstein. Steinkohl. Wettin u. Lobejun., 1847, fas. 4, p. 47, t. 20 
 
 ; ar Sternberg, Flora, ii., p. 50, t. 12. 
 .s ee Ten. Woods, Journ. R. Soc. N. S. Wales for 1882 [1883], p. 188. 
 HA * Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1888, viii., Pt. i., p. 84. 
 
 Obs. The roots and stems are described by the Rev. J. E. Tenison Woods as 
 of common occurrence at the undermentioned locality, but the leaves are rare. He says, 
 “They abound in the strata, and there are some portions of the stone which seem to 
 be made up entirely from the stems.” These examples have not come under my 
 notice. 
 
 Loc. and Horizon. Bogantungan, Drummond Range (The late Rev. J. H. T. 
 Woods)—Star Beds. 
 
 CALAMITES, sp. ind. 
 
 Obs. The occurrence of so typical a Carboniferous plant as Calamites, amongst 
 other genera, associated with a Carboniferous marine fauna in Eastern Australia, has, so 
 far, been a point of considerable doubt and controversy. Lepidodendron has already 
 been recorded,* irrespective of the facts given in these pages. Of the two species 
 known in Australia, one, Calamites (Asterocalamites) scrobriculatus, besides its Queensland 
 habitat, occurs in the Lower Carboniferous of New South Wales, whilst C. varians is of 
 doubtful horizon in the same country. In the specimen now about to be referred to, 
 we have a plant from the Rockhampton Training Wall Quarries, which have yielded 
 a rich Permo-Carboniferous fauna to the researches of Messrs. De Vis and the late 
 James Smith, partaking of many of the characters of the genus Calamites. 
 
 The stems are long, narrow, parallel-sided, and not increasing in width, oval in 
 section arising from compression, and producing a gently convex surface. The longest 
 of the specimens is nine inches in length, with an average width of one and a-half inches, 
 although one of the fragments is nearer two inches. The internodes are of irregular 
 
 
 
 * Ann. Report Dept. Mines N. 8. Wales for 1889 [1890], p. 239. 
 
189 
 
 length, the longest being about three inches and the shortest an inch and a-quarter. 
 The nodes, although faintly marked, are sufficiently so to demonstrate the generic 
 identity of the plant, and are very apparent on the application of the finger, but 
 the pressure which the specimens have undergone renders them rather oblique. The 
 coste, or ribs, are fine, narrow, and close together, opposite on contiguous internodes, 
 and not alternating. ‘The fineness of the coste probably indicates that the bark, when 
 present, entirely concealed them, whilst the continuity of the cost from internode to 
 internode indicates Areheocalamites as the section to which the plant should be referred. 
 There are no scars of branches along the nodes, as in either Calamitina, Hucalamites, or 
 Stylocalamites. 
 
 The whole of the organic matter has been removed, the specimens being merely 
 the infilling by matrix of the cavity left by the decomposition of the plant. 
 
 Loc. Lower Training Wall Quarries, Fitzroy River, Rockhampton (The late 
 James Smith). 
 
 Genus—ASTEROCALAMITES, Schimper, 1862. 
 
 (Terr. Transition des Vosges, p. 321.) 
 
 ASTEROCALAMITES SCROBICULATUS, Schlotheim., sp., Pl. 4, figs. 11, 12. 
 
 Calamites scrobiculatus, Schl., Petrefactenkunde, 1820, Abth. 1, p. 402, t. 20, f. 11. 
 pe radiatus, Brongniart, Hist. Foss. Vég., 1828, p. 122, t. 26, f. 2. 
 Ae radiatus, Feistmantel, Palaeontographica, 1879, Supp. Bd. iii., Lief. 3, Heft 4, p. 144, t. 6, f. 1, 
 t. 7, ff. 3, 4. 
 £ sea Ten. Woods, Journ. R. Soc. N.S. Wales for 1882 [1883], xvi., p. 187, t. 11, f. 5, t. 12, 
 fia (aks 
 4 Dae Ten. Woods, Proc. Linn. Soc. N. 8S. Wales, 1883, viii., Pt. 1, pp. 52, 83. 
 Asterocalamites scrobiculatus, Kidston, Cat. Foss. Plants, Brit. Mus., 1886, p. 35, 
 
 Obs. This species is quoted as a Queensland plant by the Rev. J. E. Tenison 
 Woods at one part of his Paper on the “Fossil Flora of the Coal Deposits of 
 Australia,’ but is not described in that portion devoted to the specific diagnosis. 
 My Colleague, however, quotes Calamites radians * from a definite locality in Queens- 
 land, and this may perhaps be meant for the same species. Good examples have 
 been collected by Mr. W. Fryar, Inspector of Mines, from Bogantungan, correspond- 
 ing well with Mr. Woods’ figures. One of these exhibits five nodes and the other 
 three. 
 
 Loc. and Horizon. Bogantungan, Drummond Range (W. Fryar) ; ? Drummond 
 Range (&. LZ. Jack)—Star Beds. 
 
 Family—SCHIZONEURID. 
 
 Genus—PH YLLOTHECA, Brongniart, 1828. 
 (Prodrome Hist. Vég. Foss., p. 151.) 
 
 PHYLLOTHECA AUSTRALIS, Brongniart, Pl. 17, f. 13. 
 Phyllotheca australis, Brong., loc. cit., p. 152. 
 
 o- ne Morris in Strzelecki’s Phys. Descrip. N. 8. Wales, &c., 1845, p. 250. 
 a5 - Dana, Geology Wilkes’ U. S. Explor. Exped., 1849, p. 718, t. 13, f. 6, t. 14, £ 1. 
 * re Feistmantel, Palaeontographica, 1878, Supp. Bd. iii., Lief. 3, Heft 3, p. 83, t. 6, f. 3, 
 
 1, 7, £1, 2, t. 15;f. 1 and 2 (2): 
 
 Obs. This plant is a very characteristic fossil of the Freshwater Beds of the 
 Bowen River Coal Field Series. Some years ago I wrote on this pvint “that the 
 
 
 
 * Handbook of Queensland Geology, 1886, p. 41. 
 
190 
 
 remains are almost wholly those of plants, chiefly consisting of Glossopteris and Phyllo- 
 theca.” The Revd. J. BK. T. Woods recorded Phyllotheca (P. indica ?) from the Oaky 
 Greek Coal Field and the Burrum River Coal Beds,* but in a later publication he says, t 
 “T now wish to state that, after a careful examination, there is no evidence that 
 these specimens belong exclusively to Phyllotheca.” As, however, my Colleague 
 regards the Oaky Creek Coal Beds as the equivalents of the Freshwater Series at 
 Bowen, it is not improbable that a Phyllotheca does occur there in company with 
 Glossopteris. A small specimen is figured (PI. 17, fig. 18) and, although not very 
 perfect, it corresponds with one of Dana’s illustrations.{ It was identified by Mr. R. 
 Kidston. 
 
 Phyllotheca australis, like Glossopteris Browniana, is one of the few plants which 
 pass from the Paleozoic into the Mesozoic plant-bearing beds of Eastern Australia. 
 Dr. Feistmantel has remarked on this fact in the following words: “ This species has in 
 Australia a distribution from the Lower Coal Measures . . . . into the Upper 
 Mesozoic Beds of Queensland and Victoria.” 
 
 Loc. and Horizon. Cockatoo Creek, twelve miles up (&. L. Jack)—Upper or 
 Freshwater Series of the Bowen River Coal Field. 
 
 Order—FILICES. 
 Family—SPHENOPTERIDE.§ 
 
 Genus—SPHENOPTERIS, Brongniart, 1822. 
 (Mem. Mus. Hist. Nat. Paris, viii., p. 233.) 
 
 SPHENOPTERIS LOBIFOLIA, Jlorris. 
 
 Sphenopteris lobifolia, Morris in Strzslecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 246, t. 7, ff. 3, 3a. 
 8 FP Feistmantel, Palaeontographica, 1878, Sup. Bd., iii., Lief. 3, Heft 3, p. 87. 
 p = Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., Pt. 1., p. 88. 
 
 Obs. ‘This species is described as a very delicate fern, with very slender pinnules, 
 varying much in shape according to position. 
 
 Loc. and Horizons. Near Cracow Creek, Dawson River (The late R. Daintree)— 
 ? Middle Series, Bowen River Coal Field; Rosella Creek, two miles above Havilah- 
 Byerwin Road-crossing (2. L. Jack)—Marine Bed intercalated with the Upper or 
 Freshwater Series, Bowen River Coal Field; Bowen River District (Rev. J. #. T 
 Woods ; Colln. Woods)—Middle Series, Bowen River Coal Field ? 
 
 SPHENOPTERIS FLEXUOSA, WcCoy. 
 
 Sphenopteris flexuosa, McCoy, Ann. and Mag, Nat. Hist., 1847, xx., p. 150, t. 9, ff. 4, 4a. 
 = af Feistmantel, Palaeontographica, 1878, Supp. Bd. iii., Lief. 3, Heft 3, p. 88. 
 - 5 Tenison Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., Pt. 1, p. 91. 
 
 Obs. A very graceful fern has occurred, thickly covering altered shale from the 
 Dawson River, and associated with Glossopteris. It possesses the elongately lobed 
 pinnules of this species, the characteristic forked venation, and the terminal trilobed 
 division. 
 
 
 
 * Proc. Linn. Soc. N. S. Wales, vol. viii., p. 95, 
 
 + Fossil Flora of the Coal Deposits of Australia. Sydney, 1883, p. 38. 
 
 PUD ana LOC. Cites ualer, 1. Os 
 
 §In addition to this family we believe we have the Pecopteride represented in specimens from 
 Walker’s Creek, near Nebo, and Dinner Creek, Stanwell. In each case the Pecopterid plant is accompanied 
 by Glossopteris Browniana, Brong, 
 
191 
 
 The Rev. J. E. Tenison Woods does not quote this species as a Queensland fern, 
 but in its place records the above species S. lobifolia from near Cracow Creek, Dawson 
 River. This is, of course, quite possible ; but after a very careful examination of the 
 present specimens, assisted by Mr. T. Whitelegge, my Colleague in the Australian 
 Museum, I can come to no other conclusion than that 9. feawosa must also be added to 
 the list. 
 
 Loe. and Horizon. Dawson River (H. Mackay; Colln. De Vis)—Upper or 
 Freshwater Group of the Bowen River Coal Field. 
 
 SPHENOPTERIS CREBRA, Zen. Woods ? 
 Sphenopteris crebra, Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, viii.. Pt. 1, p. 98, 6. 3, f. 4. 
 
 Sp. Char. Frond evidently tender and membranaceous, bipinnate ; pinne wide, 
 alternate, slightly oblique, oblong-quadrate, pinnules so close together as not to be 
 easily distinguished, faintly pinnatifid; lobes a little more oblique than the pinne, 
 oblong-ovate, with a slightly undulating margin; costwe sending off veins which fork 
 once, and the venules reaching the margin. (Zen. Woods.) 
 
 Obs. Specimens before me are not sufficiently perfect to show the pinne, but, 
 so far as one can judge from the brief characters of the pinnules, and the indistinct 
 figure, they are the above species. The pinnules are quite close together, almost over- 
 lapping in places, but this may be due, perhaps, to some extent to pressure ; oblong- 
 ovate in outline, and with practically an entire margin. The veins fork only once, and 
 all the venules reach the margin; of the former there are three on each side the 
 midrib to the pinnule. 
 
 Our specimens are distinguished from Sphenopteris exilis, Morris, 8. lobifolia, 
 Morris, S. germanus, McCoy, 8. flexuosa, McCoy, and S. plumosa, by the almost entire 
 margins of the pinnules; from S. hastata, McCoy, by the differently formed pinnule, 
 the latter in the present examples varying from oval-pyriform to oblong-ovate. Mr. 
 Woods speaks of the lobes of the pinnules, but if these are to any extent developed in 
 the Ballimore Coal Field examples, our Queensland fossils must then be considered 
 distinct, for the pinnules in the latter would certainly not come under this category. 
 
 Loc. and Horizon. Dawson River (H. Mackay; Colln. De Vis)—Upper or 
 Freshwater Group of the Bowen River Coal Field. 
 
 Family—PALAOPTERIDEA. 
 
 Genus—ANEIMITES, Dawson, 1860. 
 (Quart. Journ. Geol. Soc., xvii., p. 5.) 
 
 ANEIMITES AUSTRINA, Etheridge fil. 
 Aneimites austrina, Etheridge fil., Proc. Linn. Soc. N.S. W., 1888, iii., Pt. 3, p. 1804, t. 37. 
 
 Sp. Char. Frond elongately expanding, bipinnate; rachis moderately broad, 
 carinate ; pinne sub-alternate, elongate, attenuating but slowly towards their apices, 
 almost parallel-sided ; rachis carinate, frequently zigzag; pinnules petiolate, rather 
 inequilateral, varying in shape on different parts of the frond, but generally ovate or 
 obovate-pyriform, sometimes a little sub-imbricate, proximal or inner margins parallel 
 to the rachis, upper and distal margins broadly rounded, and all entire; pinnules 
 towards the apices of the pinne becoming more truly pyriform or pyriform-deltoid, the 
 terminal leaflets being uni-, bi-, or tri-lobed; pinnules of the lowest (preserved) pinne 
 lobate, the apical lobe more or less lanceolate. Petioles short and straight. Nerves 
 well marked, numerous, bi- or perhaps tri-dichotomous. 
 
192 
 
 Obs. The relation of this plant is with the group of ferns represented by such 
 genera as Cyclopteris, Archeopteris (—=Paleopteris), Rhacopteris, Adiantites (so-called), 
 and others. The resemblance is specially strong to Cyclopteris and Adiantites, but I 
 believe Professor Géppert, the author of the latter, abandoned his genus in favour of 
 Cyclopteris. 
 
 In originally proposing Ane‘mites,* Principal Dawson evidently had in mind the 
 British Coal Measures fern, Sphenopteris adiantoides, Lindley and Hutton; so much so 
 that to this he at first referred the plant afterwards called by him Aneimites (Cyclop- 
 teris) acadica.t 
 
 This being the case, we may justly include Sphenopteris adiantoides in Aneimites. 
 Furthermore, it is to be regretted that Principal Dawson did not refer to this obvious 
 fact in his second and more detailed account of the Canadian fern. 
 
 The strong resemblance borne by the Queensland specimen to the British 
 Aneimites adiantoides, L. and H., sp., and in a less degree to A. acadica, Dn., renders it 
 exceedingly probable that it should be placed in the genus in question. I shall, there- 
 fore, speak of it in future as Aneimites austrina. 
 
 The pinne of A. austrina are about three inches long, the entire frond, as 
 preserved, occupying a space of more than one foot. The frond is generally flabellate 
 and bipinnate, there being portions of eight pinne on one side, alternating with seven 
 on the other, of a rather broad rachis.- The pinne are elongate and generally narrow, 
 hardly expanding from a uniform width, and decreasing but very slowly in width towards 
 their apices. The pinnules are ovate or obovate-pyriform, and retain their form 
 throughout the length of each pinna until near their apices, when the pinnules 
 become longer and more wedge-shaped, the pinna terminating in a uni-, bi-, or 
 tri-lobed pinnule. The pinnules have likewise a somewhat flabellate aspect, seldom 
 sub-imbricate, or overlapping one another, but separated by an interspace, which is 
 certainly at times rather inconspicuous. The proximal margins of the pinnules are 
 parallel to the rachis, and during fossilisation some of them have slightly infringed on 
 the latter. 
 
 The two lowest pinne exhibit a marked difference from those above them. The 
 second pair are the best preserved and are deeply lobate and pinnatifid, conforming to 
 the habit we are accustomed to associate with the pinnules in some Sphenopterids. The 
 divisions of the pinne in question have quite lost their pyriform or obovate outline, but 
 are irregularly trilobate, and ‘to some exteni incised, the apical lobe being the largest, 
 and more or less lanceolate. The nerves are but faintly visible on the specimen 
 occupying the greater portion of the slab, but are shown on a smaller example lying 
 near. The lower pinne seem to be only a modification of the lobate apical pinnules of 
 the higher pinne, as seen on the third to the right from the bottom of the specimen, 
 and the fifth and sixth on the left hand. But they are not the basal, as the lower 
 portion of the frond is concealed by matrix. 
 
 The resemblance of A. austrina to A. adiantoides consists in the similar obovate 
 or pyriform pinnules, with a like modification of the apical pinnules. The two ferns, 
 however, differ greatly in the relative sizes of their respective portions, whilst in the 
 British species there is no appearance of the dissimilar lower pinne. 
 
 From A. acadica, Dn., the form of the pinnules will at once distinguish it. 
 
 Loc. and Horizon. Near Mount Budge, Drummond Range (A. EH. Holmes ; 
 Colln. Smith)—Star Beds. e 
 
 
 
 * Quart. Journ. Geol. Soc., 1860, xvii., p. 5. 
 
 + The Fossil Plants of the Lower Carboniferous and Millstone Grit Formations of Canada. Geol. 
 Surv., Canada, 1873, p. 26, 
 
193 
 
 Family—DICTYOTANIOPTERIDE, 
 
 Genus—GLOSSOPTERIS, Brongniart, 1828. 
 (Prodrome Hist. Vég. Foss., p. 54.) 
 
 Obs. Besides the Permo-Carboniferous localities in which different species of 
 this genus afterwards referred to have been discovered, the genus also occurs in the 
 Desert Sandstone. 
 
 That the plants discovered at Cement Hill, near Clermont,* are Glossopteris 
 there can be no reasonable doubt, but I must be allowed to consider my Colleague and 
 his Assistant, Mr. W. H. Rands, as wholly responsible for the reference of the beds 
 from which the specimens come, to the upper member of the Queensland Cretaceous, 
 the Desert Sandstone.+ The case is, however, a parallel one to the supposed occurrence 
 of Glossopteris in the Cretaceous of Russia, or the Tertiary rocks of Italy ;{ but in 
 these cases there is an element of doubt whether or no the leaves in question are truly 
 those of Glossopteris. | 
 
 The Clermont plants came to hand too late for description in these pages, but 
 they will appear amongst supplementary descriptions of Queensland fossils. 
 
 GLOSsOPTERIS BROWNIANA. 
 
 Brongniart, Pl. 16, figs. 6 and 8; Pl. 17, figs. 9 and 10. 
 Glossopteris Browniana, Brong., Hist. Vég. Foss., 1828, p. 223, t. 62. 
 
 ne 5 Morris in Strzelecki’s Phys. Descrip. N. 8. Wales, 1845, p. 247, t. 6, f. Land la. 
 A 48 Dana, Geology Wilkes’ U. S. Explor. Exped., 1849, p. 716, Atlas, t. 12, f. 13. 
 a 55 Feistmantel, Palaeontographica, 1878, Sup. Bd. iii., Lief. 3; Heft 2, p.78; Heft 3, 
 
 p: 90, 6.8, f. 3iand 4, t. 19; f. 1, 1a, 3, 4, and’4@, 5 and 5a, 7, t. 11, £. 1. 
 
 Obs. This much abused and disputed plant is very characteristic, in Queensland, 
 of the equivalents of the Upper Coal Measures of New South Wales. Itis, undoubtedly, 
 associated with the coal-seams of the Cooktown area, and on the specimens submitted 
 to him from this locality Mr. Robert Kidston makes the following remarks :—‘ Among 
 the specimens are some which may perhaps be referred to the variety australasica of 
 Brongniart. Schimper mentions in his Zvraité de Pal. Veg. (vol. i., p. 646) that 
 the form of the fronds varies much according to their age, and that he had seen 
 on the same slab some that were almost linear, and others that were oblong- 
 spathulate.”’ 
 
 G. Browniana occurs in the Upper or Freshwater Series of the Bowen River 
 Coal Field, which, like the Middle or Marine beds, possesses a Paleozoic fauna, but in a 
 less degree. On the subject of the Marine bands in the former, I formerly made the 
 following remarks :— 
 
 “The Marine bed at Rosella Creek contains Goniatites micromphalus (Morris) and 
 some indeterminable fragments of other Mollusca. The similar bed at the Havilah- 
 Byerwin Road contains magnificent specimens of a particularly characteristic Carbon- 
 iferous Brachiopod Derbyia senilis, Phillips, in company with Productus brachytherus, 
 G. Sowerby, and a bivalve, either a Pachydomus or Astartila. 
 
 Striking confirmation is again afforded by yet another locality, Cockatoo Creek, 
 where we have Glossopteris and Phyllotheca actually in company with Strophalosia 
 Clarkei, Eth.” 
 
 * See p. 169. = 
 
 + What I said (sce p. 170) was that beds in which G@lossopteris occurs, unaccompanied by other fossils, 
 ‘may be of any age from the Lower” [I should have said ‘‘ Middle ”] ‘‘ Bowen to the Desert Sandstone.” 
 (R.L.J.) : 
 +t Feistmantel, Geol. Pal. Relations Coal and Plant-bearing Beds of E. Australia, Mem, Geol, 
 Survey N. S. Wales, Pal. No. 5, 1890, p. 119, 
 
 N 
 
 
 
194: 
 
 My Colleague’s testimony on this subject is of the highest value. He says in con- 
 nection with a Bore (No. 1) put down on Pelican Creek through the Middle or Marine 
 Series—“ The most interesting feature of this bore, is the presence, at the base of the 
 Marine Series, of a considerable thickness of strata, containing Glossopteris, and 
 undoubtediy on a lower horizon than the sandstone overlying the Garrick seam, which 
 contain marine fossils.””* This would appear to entirely corroborate the previously 
 expressed opinion of the late Mr. Daintree on the occurrence of Glossopteris in tho 
 Bowen Marine Series.+ 
 
 In our illustrations we have given more than one vanety of this fern. In 
 Pl. 16, figs. 6 and 8, are two very finely reticulated leaves resembling a figure by 
 Feistmantel t and another by Morris.§ In Pl. 17, fig. 9, is a somewhat coarser 
 form, but fig. 10 of the same plate seems to represent the true variety intended 
 by Brongniart, under the name of awstralasica || with a coarser and more open 
 reticulation. 
 
 Loc. and Horizon. MacArthur Creek, below MacArthur Coal-Seam ; Cockatoo 
 Creek, three and a-quarter, eleven, and twelve miles up, Bowen River Coal Field 
 (R. L. Jack); Walker's Creek, near Nebo (2. Z. Jack); Stewart’s Creek, near 
 Townsville (R. Z. Jack); Dinner Creek, Stanwell (Lhe late James Smith) ; Dawson 
 River (H. Mackay; Colin. De Vis)—Upper or Freshwater Series (Upper Coal 
 Measures of New South Wales). 
 
 G. Browniana has been recognised by Mr. Robt. Kidston in later Collections 
 of Mr. Jack’s from Dave Creek, Little River, Cooktown; from a parting in a coal- 
 seam at the Little River, Cooktown; from impure coal, south of the ‘forty-five 
 acre seam;”’ from “ Built-up sidling” on old road from Daddy’s to Deep Creek, Cook- 
 town. Mr. Kidston has also determined a Glossopteris from the right bank of 
 the Little River, half-a-mile below Fairlight Station, Cooktown, and also from 
 Baird’s Mine, Oakey Creek, on which he remarks—‘“ The specimens are too imperfect 
 for specific determination, but probably most of them are referable to Glossopteris 
 Browniana.” 
 
 GLOSSOPTERIS LINEARIS, McCoy, Pl. 18, fig. 14. 
 Glossopteris linearis, McCoy, Ann. and Mag. Nat. Hist., 1847, xx., p. 151, t. 9, f. 5 and 5a. 
 
 Feistmantel, Palaeontographica, 1878, Supp. Bd. iii., Lief. 3, Heft 3, p. 91, t. 8, f. 1 
 and 2, t. 11, f. 3 and 4, t. 12, f. 4. 
 
 33 
 
 Obs. This species has been identified by Mr. Kidston amongst my Colleague’s 
 gatherings from the Oakey Creek Coal Field. In New South Wales it occurs in the 
 Newcastle Coal Field, at Woollongong, and other places. In the Bowen River District, 
 G. linearis is found associated with Phyllotheca and Strophalosia Clarkei, and is further 
 confirmatory evidence of the occurrence of this interesting genus in company with 
 Paleozoic Mollusca. In Pl. 16, fig. 4, the neuration would appear to spring from the 
 midrib at too near a right angle to fully correspond with the recognised figures of this 
 species. 
 
 Loe. and Horizon. Cockatoo Creek, Bowen River Coal Field (R. ZL. Jack) ; 
 Baird’s Mine, Oakey Creek Coal Field, Cooktown (2. L. Jack)—Upper or Fresh- 
 water Series of the Bowen River Coal Field. 
 
 
 
 * Handbook Geol. Queensland, 1886, p. 44. 
 
 + Quart. Journ. Geol. Soc., 1872, xxviii., p. 286. 
 + Palaeontographica, loc. cit., t. 10, f. 5. 
 
 § Strzelecki, /oc. cit., t. 6, f. 1. 
 
 || Brongniart, loc. cit., t. 62, f. 1. 
 
195 
 
 GLOSSOPTERIS AMPLA, Dana, PI. 15, fig. 7. 
 
 Glossopteris ampla, Dana, Geology Wilkes’ U. S. Explor. Exped., 1849, p. 717; Atlas, t. 138, f. 1. 
 Feistmantel, Palaeontographica, 1878, Supp. Bd. iii., Lief. 3, Heft 3, p. 91, t. 11, f. 2, 
 tot ie 
 
 Obs. The discovery of this fern in Northern Queensland, associated with a 
 Paleozoic fauna, may be regarded as one of the most important paleontological facts 
 brought to light by my Colleague’ ssurveys. It entirely corroborates the often-repeated 
 statements of the late Revd. W. B. Clarke and Mr. W. Keene that @lossopteris, whatever 
 its statigraphical position might be in other countries, was associated with Palszozoic 
 Marine beds in New South Wales. I cannot do better than quote here the remarks I 
 originally made when first recording the appearance of this fern in company with 
 Paleozoic shells in the Upper or Freshwater Series of the Bowen River Coal Field :— 
 
 “In the case of the Coral Creek deposit, we have an assemblage of fossils most 
 carefully collected, and all presenting traces of one and the same matrix. An 
 undoubted Glossopteris occurs here, near G. ampla, Dana, in company with Polyzoa of 
 an Upper Paleozoic type, such as Fenestella, Protoretepora, two species of Stenopora, a 
 specimen which is either Productus or Strophalosia, probably the latter; bivalves of 
 the genera Pachydomus and Me@onia, another which I cannot distinguish from Aviculo- 
 pecten limeformis, Morris, and certainly Pterinea macroptera, Morris. An assemblage 
 of fossils such as this would have been considered by all those who have in previous 
 years written on the subject, Professors Morris, McCoy, Dana, and Jukes, Mr. Daintree 
 and others, as representing the Upper Paleozoic Series of New South Wales, &c. 
 
 “Ina Presidential Address delivered to the Royal Society of Victoria on the 25th 
 April, 1864,* Professor McCoy tells us that in a discussion which took place at the 
 reading of a Paper by Mr. Daintree, the latter mentioned ‘a fact of the highest 
 importance, and which may be found in some measure to reconcile the view of Mr. 
 Clarke and myself, namely, that Mr. Clarke in making his original collections for 
 determination had mixed together the fossils of the upper and the lower beds. Now, 
 as a portion of the fossils could be identified with European-species, and there were 
 among them two species of Trilobites (Phillipsia and Brachymetopus), characteristic 
 of the Mountain Limestone as found in Ireland and Russia, the clearly marked age of 
 these would have determined the age of the whole, if, as was supposed, they came from 
 the same beds; and in this indirect way the Pachydomi and other new generic 
 and specitic forms which, from their novelty, could not afford any indication of age of 
 themselves, came to be considered as Paleeozoic forms from their supposed associations 
 with those which certainly were of that age. It is obviously, therefore, necessary to 
 collect and investigate the evidence afresh from each bed by itself with care,’ &c. 
 These remarks, although undoubtedly sound in principle, will not apply in this case, for 
 we have here careful collecting, showing that Glossopteris does actually exist in a 
 deposit with a marine fauna, amongst which is at least one specimen of Productus or 
 Strophalosia. Further, the same species of Polyzoa which are found in abundance in 
 the Coral Creek deposit with the Glossopteris are also met with at Pelican Creek, 
 where the characteristic fossil is Strophalosia Clarke. 
 
 “Taking all these facts into careful and unbiassed consideration, it appears to 
 me impossible to doubt, if the Coral Creek fauna is admitted to be of Permo- 
 Carboniferous age, or, at any rate, of Upper Paleozoic, that we now have a tangible 
 demonstration of the occurrence of Glossopteris in actual company with such a fauna.” 
 
 Loc. and Horizon. Coral Creek, Bowen River Coal Field (2. L. Jack)—Middle 
 or Marine Series. 
 
 Led 
 
 
 
 * Trans, R, Soc. Vic., 1865, vi., p. Ixvi, 
 
196 
 
 Order—LYCOPODIACEE, 
 Family—LEPIDODEN DRIDZ. 
 Genus—LHPIDODENDRON, Sternberg, 1820. 
 
 (Flora der Vorwelt, i., Fasc. i., p. 25, Fasc. 4, p. x.) 
 
 LEPIDODENDRON AUSTRALE, McCoy, Pl. 5, figs. 1-10. 
 Lepidodendron (Bergeria) australe, McCoy, Prod. Pal. Vict., Dec. i., 1874, p. 37, t. 9. 
 
 “f nothum (pars.), Carruthers (non Unger), Quart. Journ. Geol. Soc., 1872, xxvili., Pt. 3, p, 353, 
 t. 26, f. 11-14 (excl. figs. 1-4, 6-9). 
 
 MG nothum, Feistmantel, Palaeontographica, 1878, Supp. Bd. iii., Lief. 8, Heft 2, p. 69, t. 1, 
 f. 1-5 ; Ibid, 1879, Heft 4, p. 141, t. 1 (19), f. 1 and 2. 
 
 es australe et L. nothum, Ten. Woods, Proc. Linn. Soc. N.S. Wales for 1883 [1884], viii., 
 
 Pt. 1, pp. 184 and 185. 
 
 Obs. Both Mr. Robert Kidston and the Writer are quite in accord with Prof. 
 McCoy in considering the plant described by Mr. Carruthers under the name of 
 Lepidodendron nothum, Unger, as identical with ZL: australe, MeCoy.* Mr. Kidston 
 remarks in his notes on the Queensland plants :—‘‘ The type of Lepidodendron nothum, 
 Unger, on account of its imperfect preservation does not appear to afford any specific 
 character from external markings, by which other specimens can be satisfactorily identified 
 with it; therefore the identification of the Queensland or Tasmanian specimens with 
 ' Unger’s plant does not appear admissible.” Prof. McCoy remarks that ‘‘ The scars are 
 so much larger and fewer on approximately the same sized branches”’ (7.e., of L. 
 australe), ‘“‘that it is not desirable to make such a reference”’ (z.e., to LZ. nothum, 
 Unger). Lepidodendron nothum, Carruthers (non Unger), is believed by Mr. Kidston to 
 include two species, belonging in part to Z. australe, McCoy, and in part to Leptophlewm 
 rhombicum, Dawson.t According to this view, Mr. Carruthers’ figures (PI. 26, loc. cit., 
 figs. 11-14), must be referred to Z. australe, and the remainder given on his plate 
 (figs. 1-4, 6-9) to Leptophleum rhombicum. The differences in the form of the leaf-scar, 
 the position of the vascular cicatricule, and mode of growth of these specimens, seems to 
 prohibit their being included in one species.”’ The latter figures have a great resemblance 
 to Leptophleum rhombicum in the form of the scar and position of the cicatricule. 
 
 Loc.and Horizon. Corner, Sandy, Horse, and Donald’s Creeks, Great Star River 
 (R.L. Jack and P.W. Pears); Road to Harvest Home, two miles west of Mount McConnell 
 (P. W. Pears) ; Mount Wyatt, Canoona, Broken River (The late R. Daintree) ; Medway 
 River, Bogantungan, and Drummond Range (Lhe late Rev. J. H. T. Woods)—Star Beds ; 
 Training Wall Quarries, Rockhampton, with marine mollusea (The late James Smith) ; 
 
 Murphy’s Tunnel, Pioneer Hill, Hodgkinson Gold Field (R. L. Jack)—Gympie Beds. 
 
 LEPIDODENDRON VELTHEIMIANUM, Sternberg, Pl. 4, fig. 8, Pl. 6, fig. 2. 
 Lepidodendiron veltheimianum, Sternberg, Flora der Vorwelt, 1870, i., Fasc. 4, p. xii., t. 52, £. 3. 
 
 a a Feistmantel, Palaeontographica, 1879, Bd. iii., Lief. 3, Heft 4, p. 151, t. 7, 
 f, 2'(? t. 5, ff. 2 and 3). 
 
 3 55 Ten. Woods, Journ. R. Soc. N. S. Wales for 1882 [1883], xvi., p. 182. t. 11, 
 Lmli3; and 6, coal oentna. 
 
 56 rs Ten. Woods, Proc, Linn. Soc. N. 8S. Wales, 1883, viii., Pt. 1, p. 185. 
 
 Obs. This Lycopod was recorded as a Queensland species by the late Rev. 
 
 J. E. Tenison Woods. It occurs as compressed branches, with impressions of distant 
 narrow-pointed leaf-like scales. 
 
 
 
 * For a full discussion of the relation of these two plants see my Paper—Lepidodendron australe, 
 
 McCoy : Its Synonyms and Range in Eastern Australia. Records Geol. Survey N.S. Wales, 1891, ii., Pt. 3, 
 pp. 119-134. (R. #., junr.) 
 
 + Denkschr. Akad. Wiss. Wien, xi., 1856, p. 175, Pl. x., f. 4-8. 
 
 ~ Geol, Surv., Canada, Foss, Plants, Dev. and Up. Silurian Form, Canada, 1871, p, 36, t. 8, figs. 88 
 and 89, 
 

 
 107 
 
 Two good examples are included in my Colleague’s Collection, showing the 
 elongated, narrow, and long diamond-shaped scars characteristic of the species. ‘These 
 are accompanied by examples of the Knorria condition (Pl. 6, f. 2). 
 
 Loc. and Horizon. Drummond Range (R. Sexton and the late Rev. J. E. 
 Lenison Woods); Bogantungan, Drummond Range (W. Fryar)—Star Beds. 
 
 LEPIDODENDRON, sp. ind., Pl. 6, figs. 1 and 4. 
 
 Obs. A third, and perhaps even a fourth, species of Lepidodendron is repre- 
 sented by the above figures. In both cases the scars have been rendered too plainly 
 by the Artist. For want of sufficient material I have not attempted to determine 
 them. 
 
 Loc. and Horizon. Bogantungan, Drummond Range (W. Fryar); Corner 
 Creek, Great Star River (P. W. Pears)—Star Beds. 
 
 Genus—CYOLOSTIGILA, Haughton, 1860. 
 (Ann. and Mag. Nat. Hist., 1860, v., p. 443.) 
 
 CYCLOSTIGMA AUSTRALE, Feistmantel. 
 
 Cyclostigma australe, Feist., Palaeontographica, 1878, Supp. Bd. iii., Lief. 3, Heft 2, p. 76, t. 4, f. 3, t. 5, 
 ale 
 45 sp., Ten. Woods, Journ. R. Soc. N. S. Wales for 1882 [1883], xvi., p. 184. 
 ) australe, Ten. Woods, Proc. Linn. Soc. ‘bid., 1883, viii., Pt. 1, pp. 52 and 138. 
 Obs. The late Rev. J. E. T. Woods obtained a specimen from the Drummond 
 Range which he thought might be this species. 
 Loe. and Horizon, Drummond Range (The late Rev. J. EL. T. Woods)—Star 
 Beds. f 
 
 CrcoLostiema, sp. did. 
 
 Cyclostigma, sp., Feistmantel, Palaeontographica, 1878, Supp. Bd. iii., Lief. 3, Heft 2, p. 71. 
 a vs Journ. R. Soc. N. 8. Wales for 1880 [1881], xiv., p. 116. 
 
 Obs. A plant very closely allied to Cyclostigma kiltorkense is said by Dr. Feist- 
 mantel to occur in Queensland in company with Lepidodendron nothum (L. australe, 
 McCoy), but it may possibly be the last species only. 
 
 Loc. and Horizon. Mount Wyatt and Canoona (Dr. O. Feistmantel)—Star 
 Beds. 
 
 Genus—STIGMA RIA, Brongniart, 1822, 
 (Mém. Mus. Nat. Hist. Paris, viii., p. 209.) 
 
 STIGMARIA, sp. ind. 
 
 Stigmaria, Ten. Woods, Journ. R. Soc. N. 8. Wales for 1882 [1883], p. 192, t. 12, f. 8. 
 
 - Obs. The late Rev. Mr. Woods did not describe this specimen, but remarked 
 simply—“This fragment lay in the position of a root in the rock, subtending a stem 
 probably of Lepidodendron veltheimianum.” 
 
 Loe. and Horizon. Bogantungan, Drummond Range (Lhe late Rev. J. LH. T. 
 
 Woods)—Star Beds. 
 
198 
 
 Section—PHANEROGAMIA. 
 Class—DIcOTYLEDONES. 
 Order—CYCADACEAR, 
 Family—CORDAITEA.* 
 
 Genus—CORDAITES, Unger, 1850. 
 (Gen. et Sp. Plantarum, p. 277.) 
 
 CoRDAITES AUSTRALIS, McCoy. 
 
 Cordaites australis, McCoy, Prod. Pal. Vict., Dec. iv., 1876, p. 22, t. 36, f, 6, 7. 
 - “4 Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viiil., Pt. 1, p. 155 
 
 Obs. The leaves of C. australis have been recorded by the Rev. J. E. Tenison 
 Woods from the plant beds of the Drummond Range (Star Beds). He says—‘“‘ I believe 
 I have identified the same species in the shales and slates of Gympie, Queensland (Lady 
 Mary Shaft), and also in the sandstone ranges at the Drummond Range (Bogantungan), 
 in the sandstone about one mile west of the railway station. In both it is not very 
 abundant.” The plant has not occurred in any Collection I have examined from either 
 of the above localities. 
 
 Order—CONIFERE. 
 Family—ARAUCARIE. 
 
 Genus—ARAUCAROXYLON (Krauss), Schimper, 1870. 
 (Traité Pal. Vég., 1870, ii, Pt. 1, p. 380.) 
 
 
 
 Aravucaroxyton Nicnout, Carruthers (MS.) 
 Araucaroxylon Nicholi, Carruthers in Etheridge, fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 328. 
 
 Obs. This name was given by Mr. W. Carruthers, F.R.S., to some wood obtained 
 by Mr. Jack in the Bowen River Coal Field. As Mr. Carruthers has since failed to 
 describe it, the name had better lapse, and be erased from nomenclature. It would not 
 have been referred to here had it not been necessary to account for the name, which has 
 unfortunately crept into literature. 
 
 The occurrence of Coniferous wood, however, is in itself an interesting fact, as 
 affording still further evidence of the identity of the Bowen Coal Measures with the 
 corresponding series in New South Wales. My Colleague states that in the Middle or 
 Marine Bowen beds “ portions of the trunks of coniferous trees are occasionally found 
 lying horizontally in the strata.”+ Again, in the Upper or Freshwater Series of the same 
 area, the strata exposed in Jack’s Creek contain ‘‘ numerous large drifted trees 
 (Coniferous). These occasionally retain some part of the branching roots. They are 
 silicified to a black flint, sometimes partly opalised.”{ In another place he adds—“ One 
 tree was found to measure thirty-one feet in length.’ § And what is of equal importance, 
 “the same species of drifted coniferous wood is common to the Marine and Freshwater 
 Series.’’|| 
 
 * Lesquereux, Coal Flora Carb. Form. Pennsylvania, 1880, p. 527. ‘‘The Cordaiteze are now 
 generally referred to the Dicotyledonous Gymnosperms, as intermediate in character between the Cycadacez 
 and the Conifers.” (Lesquereux.) 
 
 + Report on the Bowen River Coal Field. Brisbane: by Authority: 1879, p 7. 
 
 + Ibid., p. 22. 
 
 § Handbook Geol. Queensland, 1886, p, 45 
 
 || Report, Joc, cit. p. 35. 
 
199 
 Kingdom—ANIMALIA., 
 Sub-Kinedom—PROTOZOA. 
 
 Class—SPoNGIDA. 
 Order—MONACTINELLIDE, 
 
 Family— 
 
 Genus—LASIOCLADIA, Hinde, 1883. 
 (Cat. Foss. Sponges Brit. Mus., p. 19.) 
 
 Lastocnapra ? HInpet, sp. nov., Pl. 41, figs. 1 and 2. 
 
 Sp. Char. Form, as preserved, fan-shaped, originally globular or rotund 
 probably, measuring one and three-quarters by one and a-quarter inches, formed of 
 long, radiating, rod-like, siliceous spicules, closely compressed or matted together, 
 and apparently all placed in one outward direction. Spicules very equal in size. 
 
 Obs. The general appearance of this organism is that of a semi-circular 
 or fan-shaped body, split in half longitudinally on the weathered surface of an 
 indurated non-calcareous shale. To the naked eye the surface simply appears 
 roughened, but when magnified, rod-like spicules and their impressions are at once 
 apparent. Their direction is very regular, having a definite radiate arrangement, but 
 there does not appear to be any attempt at transverse or obliquely placed spicules. On 
 the bottom of the specimen, where ground down, the spicules are visible in sections, 
 which are circular and solid. All the rods seem to be simple, and are undoubtedly 
 siliceous. 
 
 This interesting form is provisionally referred to Lastocladia, Hinde, but the 
 spicules are not loosely arranged in more than one direction, as in that genus. The 
 remark of Dr. Hinde that “the larger portion of the specimen merely shows the 
 empty well-defined moulds of the spicules in the shale,” quite applies here. These 
 rods do not seem to be in any way allied to the long rope-like anchoring 
 spicules of Hyalostelia, in that they are solid, and not wholly parallel with one 
 another. 
 
 Drawings of this sponge were submitted to Dr. J. G. Hinde, who replied—“ It is 
 very probable that the specimen of which you enclose drawings is a Monactinellid 
 sponge, but further than that I can form no opinion.” Notwithstanding my friend’s 
 cautious reply, I have ventured to provisionally refer this sponge to Lasiocladia, uniting 
 with it his name. The rarity of sponges in our Australian Permo-Carboniferous 
 rocks demands that every possible attention should be called to their occurrence, 
 and no better plan can be adopted than that of giving the fossil a name. I have not 
 been able to isolate any of the spicules, and am, therefore, debarred from giving 
 measurements. 
 
 Loc. and Horizon. Rockhampton District * (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 * The fossils of the Collection received from Mr. De Vis do not bear separate localities, but are all 
 from the Rockhampton District. In a letter dated 25th July, 1888, Mr. De Vis says—-‘‘ The fossils are from 
 the Agricultural Reserve ; from the Fitzroy at Laurel Bank, about ten miles from Rockhampton, westward 
 to the Nine-mile Lagoon; thence to the Corporation Quarry, Athelstane Range, and to the northern 
 outerop (at foot of Bersekers) of the synclinal beneath the township andvbed of river.” 
 
200 
 Sub-Kingdom—CCiLENTERATA. 
 
 Class—ACTINOZOA. 
 
 The Actinozoa are but very sparingly represented in the Permo-Carboniferous 
 of Queensland and New South Wales,* and, so far as known to me, the same 
 remark is applicable to Tasmania also. ‘This applies, not only to individual genera 
 and species, but also to the orders of the class. The Zoantharia are perhaps repre- 
 sented by the genus Stenopora, whilst the Rugosa in the present collection number 
 but a few ill-preserved and undeterminable fragments. If this paucity of the 
 Coral fauna should be found to hold good in the future, as more extended 
 researches are carried out, it will, in conjunction with the repeated occurrence of 
 Stenopora, greatly assist in supporting the view here advocated of the marked 
 Permian facies of portions of the Upper Paleozoic fauna of New South Wales and 
 Queensland. 
 
 Order—RUGOSA. 
 Group—ZAPHRENTOIDEA. 
 Family—ZAPHRENTIDZ. 
 
 Genus—ZAPHRENTIS, Rafinesque and Clifford, 1820. 
 (Ann. Sci. Phys. Bruxelles, v., p. 234.) 
 
 ZAPHRENTIS PROFUNDA, sp. nov., Pl. 44, fig. 1. 
 
 Sp. Char. Corallum long and probably much curved, calice very deep, curved 
 and wide, rather more oval than circular; floor formed by a very irregular and 
 limited tabulum; a crest or callus is present on the dorsal side, and is formed by a 
 convergence of the septa. The latter are very numerous, at least forty-six primary 
 and a similar number of secondary, and pass well on to the floor; secondary septa 
 rather more than one-third the length of the primaries; septal fossula deep, imme- 
 diately under the ventral wall, bounded by two primary septa, and undivided by the 
 intrusion of the counter septum. Dissepiments very numerous, forming a close and 
 dense tissue. Depth of the calice eleven lines on the dorsal side, but one and a-half 
 inch on the ventral; longest diameter one and a-quarter inch, from the dorsal to the 
 ventral side. 
 
 Obs. This is a very remarkable species, and appears to be quite distinct from 
 any hitherto described Australian form. The large number of septa and the narrow 
 oblique calice-floor are important and definite characters. The difference between 
 the curvature of the dorsal and ventral sides is very great. The crest is situated 
 at the top of the elongated fossula, with the dorsal and ventral septa converging 
 thereto, the latter passing along the margins of the fossula; a second crest 
 occurs at the immediate entrance to the latter, which does not seem to be otherwise 
 divided. 
 
 Loe. and Horizon. Rockhampton District ¢ (C. W. De Fis)—Gympie Beds. 
 
 * For a full description of all the species known from N. 8. Wales, see my Memoir: A Monograph of 
 the Carboniferous and Permo-Carboniferous Invertebrata of New South Wales. Part 1.—Ccelenterata. 
 Mem. Geol. Survey N. S. Wales, Pal. No. 5. 4to. Sydney, 1891: by Authority. 
 
 + Sce note, p. 199. 
 
201 
 
 Group—CYATHOPHYLLOIDEA. 
 Family—CYATHOPHYLLID A. 
 Genus—CYATHOPHYLLUM, Goldfuss, 1826. 
 
 (Petrefacta Germanie, I. Theil, p. 54.) 
 CYATHOPITYLLUM, sp. ind., Pl. 3, fig. 10. 
 (Compare C. helianthoides (Goldf.), Edwards and Haime, Mon. Brit. Foss Corals, Pt. 4, Dev., 1853, p. 227, 
 t. 51, f. 1.) 
 
 Obs. <A large single corallum after the type of C. helianthoides has been found 
 at the Hodgkinson Gold Field, but too imperfect for full description. The diameter 
 across the calice was at least three inches, and in all probability much more. The 
 septa were very numerous, and a large quantity of dissepimental tissue also existed. 
 The former are too stout and not sufficiently numerous for the Carboniferous type, 
 Cyathophyllum Stutchbury?,* but are formed much more on the lines of the Devonian 
 C. helianthoides,+ and the dissepimental tissue filling the interseptal loculi also closely 
 resembles that of this species. 
 
 Loc.and Horizon. Beaconsfield, Hodgkinson Gold Field (2. L. Jack)—Gympie 
 Beds ? 
 
 CYATHOPHYLLUM, sp. ind., Pl. 7, fig. 1. 
 
 Obs. <A portion of what must have been a gigantic coral, having a diameter of 
 at least seven and a-half to eight inches, is represented in Pl. 7, fig. 1. The figure 
 displays a natural section taken horizontally from the radial centre outwards to the 
 circumference or thereabouts. It is much altered by mineralization, but the septa, of 
 which there are an enormous number, are distinctly visible, and so are the dissepiments. 
 In the portion preserved, which represents only about one-tenth of the entire corallum, 
 there are forty septa, or more. This is probably one of the largest Cyathophyllcids 
 known, and it is to be regretted that more ample material is not forthcoming to enable 
 a full description to be given. It clearly belongs to the group of Cyathophyllum 
 Stutchburyi, judging from the large number of septa, and tbe close-set dissepiments. 
 
 Loc. and Horizon. Tamestone, near Langmorn, Port Curtis (W. H. Rands)— 
 Gympie Beds ? 
 
 Section—PHERFORATA. 
 Family—AULOPORIDZ. 
 
 Genus—CLADOCHONUS, McCoy. 
 (Ann, and Mag. Nat. Hist, 1847, xx., p. 227.) 
 
 CLADOCHONUS TENUICOLLIS, Me Coy. 
 
 Cladochonus tenuicollis, McCoy, loc. cit. p. 227, t. 11, f. 8. 
 Etheridge fil., Cat. Australian Foss., 1878, p. 34 (for general synonymy). 
 
 Obs. A single corallite, in Mr. De Vis’ Collection, shows the presence of this 
 coral in the Queensland Permo-Carboniferous rocks. It is on a weathered surface, but 
 does not afford any additional information to that already known. 
 
 Loc. and Horizon. Rockhampton District (C1. W. De Vis; Colln. De Vis)— 
 
 Gympie Beds. 
 
 * Edwards and Haime, Mon. Brit. Foss. Corals, Pt. 3, Carbonif., 1852, p. 179, t. 31, ff. 1 and la. 
 + Edwards and Haime, Op. cit. supra. 
 
202 
 
 Order—MONTICULIPORIDEA, 
 Family—MONTICULIPORID 2. 
 
 
 
 Genus—MONTICULIPORA, D Orbigny, 1849. 
 (Prodrome Pal., i., p. 25; Emend. Nicholson, Tab. Corals Pal. Period, 1879, p. 269.) 
 
 Monricuripora, sp. ind., Pl. 38, figs. 1 and 2. 
 
 Sp. Char. Corallum from one and a-half to two lines wide; walls of the corallites 
 thickened as they bend outwards from the imaginary axis to the surface; calices oval ; 
 intercalated cells very numerous, sometimes one row separating contiguous corallites, 
 at other times three or four rows, and forming irregular macule; spines ornamenting 
 the walls of the corallites few and irregularly disposed. 
 
 Obs. The specimen consists of a small portion of a corallum, partly in natural 
 section and partly preserved in the round. It presents all the characters of Professor 
 Nicholson’s section Heterotrypa,* and is nearly related to 1. (Helerotrypa) tumida 
 Phill. sp., especially the variety méliaria, Nicholson. Its delicate form and small size 
 assist in distinguishing this coral. 
 
 Loc. and Horizon. Kooingal, near Gladstone (Lhe late James Smith) —Gympie 
 Beds. 
 
 Genus—STENOPORA, Lonsdale, 1844. 
 
 Stenopora, Lonsdale in Darwin’s Geol. Obs. Vole. Islands, 1844, p. 161 (note). 
 as Lonsdale in Strzelecki’s Phys. Desc. New South Wales, &c., 1845, p. 262. 
 > Nicholson and Etheridge fil., Ann. and Mag, Nat. Hist., 1879, iv., p. 265. 
 $3 Nicholson, Tabulate Corals Pal. Period, 1879, p. 168. 
 Ff Waagen and Wentzel, Pal. Indica (Salt Range Foss.), 1886, Ser. xiii., vol. i., Pt. 6, p. 885. 
 a Etheridge fil., Mem. Geol. Survey N. S. Wales, Pal. No. 5, Pt. 1, 1891, p. 32. 
 
 Obs. The views held up to the present time on the structure of Stenopora will 
 be found expressed in the works and memoirs quoted above. A general account of the 
 history and structure of the genus and the Australian species will be found in the 
 “Memoirs of the Geological Survey of New South Wales,” as above indicated. 
 
 The descriptions of the three first species following is substantially the same as 
 that given by Professor H. A. Nicholson and the Writer in the “ Annals and Magazine 
 of Natural History.” 
 
 Type—Stenopora tasmaniensis, Lonsdale. 
 
 STENOPORA AUSTRALIS, Wicholson and Eth. fil., Pl. 6, figs. 5-8. 
 
 Stenopora ovata, Nich. and Eth. fil. (non Lonsdale), Ann. and Mag. Nat, Hist., 1879, iv., p. 271, f. 2a-o., 
 p. 274, t. 14, £. 1-le. 
 
 Sp. Char. Corallum sublobate or submassive, of cylindrical or flattened 
 branches, which have a diameter of from less than two to more than three centimetres. 
 Corallites vertical, or nearly so, in the centre of the branches but finally bending out- 
 ward nearly at right angles and being continued for some distance in this direction 
 before reaching the surface. Corallites in the central portions of the corallum thin- 
 walled, polygonal, and closely contiguous; but in the horizontal portion of their course 
 thickened by annular accretions, by which the tubes are placed in contact, the inter- 
 vening, unthickened segments being free. Corallites on an average about one-third 
 of a millimeter in diameter ; tubes of smaller size being here and there intercalated among 
 the larger ones. In the outer portion of the tubes, about six of the annular thickenings 
 
 * Genus Monticulipora and its Sub-Genera, 1881, pp. 101 and 108, 
 
203 
 
 of the tubes, and as many unthickened segments, occupy the space of one line. 
 Tabule horizontal, sometimes complete, or at other times perforated by a central 
 aperture, remote from one another as a general rule, and, for the most part, placed at 
 corresponding levels in contiguous tubes, these levels having no evident relation to the 
 annular thickenings of the tubes ; acanthopores wanting. 
 
 Obs. The original specimens from the Bowen River Coal Field did not exhibit the 
 surface in any manner that would enable the external characters of the species to be 
 described. In identifying them with 8S. ovata, Lonsdale, we formerly relied chiefly upon 
 the rapid divergence of the tubes from the central bundle, and the great number and 
 close arrangement of the annular thickenings of the corallites in the horizontal portion 
 of their course, these being sometimes so much developed as to give to the exterior of 
 the tubes a regularly crenulated appearance. The annular thickenings are also 
 unusually broad ; and many smaller tubes are interpolated among the larger ones as the 
 surface is approached. 
 
 In its minute structure, however, the present species differs widely from S. ovata, 
 and resembles no other species of the genus known to us. One of the most marked 
 characters of S. australis, in which it seems to stand alone among the species of 
 Stenopora, is the total absence of acanthopores (PI. 6, fig. 7). This character at once 
 distinguishes the species from S. ovata, Lonsd. It agrees with the latter in the fact 
 that the walls of contiguous corallites are completely amalgamated, the primordial wall 
 only being visible in the axis of the branches, and also in the average size of the tubes ; 
 but the corallites are mostly more of a polygonal than of a simply rounded shape. As 
 seen in longitudinal sections (PI. 6, figs. 6 and 8), the corallites are thickened periodically, 
 in the peripheral region of the corallum, by very regular fusiform thickenings placed at 
 corresponding levels in contiguous tubes, as are also the tabule. As seen in long 
 sections, the tabule appear to be complete; but, as viewed in tangential sections, 
 appearances are seen which are difficult to explain, except upon the supposition that 
 the tabule are perforated by a central aperture (PI. 6, fig. 7). Thus in many of the 
 corallites, as seen in tangential sections, we observe a broad ring of light-coloured 
 sclerenchyma internal to the proper walls of the tube, and enclosing a central rounded 
 aperture. What this ring is, unless it be a perforated tabula, it is difficult to see ; but 
 there is the curious feature that it is usually separated from the true wall for a portion 
 of its extent on one side of the tube. 
 
 In our former description of this species (loc. cit.) we described and figured the 
 above-mentioned singular structures, but were unable to give any explanation of their 
 nature, as we believed the tabul to be imperforate. We are obliged to admit, however, 
 that if this be their real nature they differ in some inexplicable points from ordinary 
 perforated tabule. In Stenopora Howsii, Nich., the tabule are not only perforated by 
 central apertures, but this fact is quite as easily recognizable in long sections as in 
 tangential ones. In this form, however, the tabule are extremely numerous and the 
 state of preservation is also very good. Mr. John Young has proposed the generic name 
 of Zabulipora for a coral allied to or identical with Stenopora Howsii. In all other 
 respects, however, save as regards its perforated tabule, §. Howszi does not differ from 
 the normal species of Stenopora. If no other species of Stenopora possessed perforated 
 tabule, there would be ground for accepting Zabulipora as a sub-genus of Stenopora, or 
 perhaps as a distinct genus. If, on the other hand, the structures above described as 
 occurring in S. australis are really perforated tabule, there does not seem to be any need 
 for a special generic name. Moreover, it is only on the supposition that perforated 
 tabule occur in the species of Stenopora generally, that we can account for Lonsdale’s 
 assertion that the mouths of the corallites in this genus are ‘‘ closed at the final period 
 
204: 
 
 of growth.” In most of the specimens we have examined (except 8. Howsiz) the surface 
 is so badly preserved that the characters of the mouths of the-tubes could not be 
 accurately determined, and in some (such as 8. ovata, Lonsd.), where the preservation of 
 the surface was better, we have not been able to recognize any such closure of the 
 mouths of the tubes. In one of the figures,* however, which Lonsdale gives of NV. 
 tasmaniensis, the structure in question is well shown, and it corresponds entirely with 
 what is seen in portions of the surface of S. Howsii, where it is undoubtedly the result 
 of the existence of perforated tabula. We have ourselves observed the same structure in 
 a single specimen of JS. tasmaniensis. 
 
 Loc. and Horizon. Coral Creek, Bowen River (&. L. Jack)—Middle or Marine 
 Series, Bowen River Coal Field. 
 
 Stenopora Lercuuarptit, Nicholson and Eth. fil., Pl. 6, figs. 9 and 10; Pl. 7, fig. 2. 
 Stenopora Leichhardtii, Nich. and Eth. fil., Ann. and Mag. Nat, Hist., 1886, xvii., p, 179, t. 8, figs, 7 and 8. 
 
 Sp. Char. Corallum dendroid, of cylindrical branching stems, which vary in 
 diameter from less than a centimetre up to one and a-half centimetre. The corallites in 
 the centre of the branches are nearly vertical, with comparatively thin walls, and 
 polygonal in shape. -In the peripheral region of the corallum, the corallites bend 
 outwards nearly at right angles to the axis, the walls becoming thickened and being 
 entirely fused with one another, while the visceral chambers become oval or rounded. 
 The periodical thickenings of the walls of the tubes in the final portions of their course . 
 are mostly long and fusiform, and are generally placed at corresponding levels in 
 contiguous corallites. The average diameter of the corallites is about one-fourth of a 
 millimetre. In the walls of the corallites, in the peripheral region, acanthopores are 
 developed in great numbers, their shape being usually oval or subangular, their size 
 large, and their walls not specially, or only slightly, thickened. ‘Tabule are very 
 sparingly developed, and are only occasionally to be recognised at all. 
 
 Obs. In its general form. this species closely resembles S. ovata, Lonsd., aad 
 the typical examples ee S. tasmaniensis, Lonsd. From these two species, Rewenen the 
 present form is distinguished, among other characters, by the extraordinary abundance 
 and large size of the acanthopores. 8. Howszi, Nich., has also very numerous acantho- 
 pores, but these arefor the most part very minute, and the annular thickenings of the 
 wall are quite different, while the tabule are very numerous, and are perforated. The 
 acanthopores are best seen in tangential sections (Pl. 6, fig. 9), but they are also well 
 exhibited in sections of the peripheral region of the corallum, cutting the corallites 
 longitudinally, in which they appear as delicate clear tubes running in the thickened 
 walls of the corallites (Pl. 6, fig. 10). Tabule are often not to be detected, and when 
 present are very few in number. In tangential sections appearances are occasionally 
 to be detected, which may perhaps be caused by the existence of perforated tabule ; 
 but.as the specimens are in a very peculiar condition of preservation, this cannot be 
 affirmed with certainty. None of our specimens exhibit the surface of the corallum, 
 and we therefore do not know if the mouths of the corallites were closed at the final 
 period of growth by the development of a perforated tabula, as seems to have been 
 sometimes the case in 8. tasmaniensis, Lonsd., and probably in S. australis, nobis. 
 
 Loc. and Horizon. Pelican Creek, half-a-mile above Sonoma Road-crossing, 
 Bowen River (&. L. Jack, and #. Hdelfelt)—Middle or Marine Series, Bowen River 
 Coal Field. 
 
 
 
 * Strzelecki’s Phys. Descrip. N. 8. Wales, &c., Pl. 8, fig. 20. 
 
205 
 
 Srenopora Jacki, Nich. and Eth. jil., Pl. 6, figs. 11-18. 
 
 Stenopora Jackti, Nicholson and Eth. fil., Ann. and Mag. Nat. Hist., 1879, iv., p. 270, f. la-c, p. 275. 
 
 A Nicholson, Tabulate Corals Pal. Period, 1879, p. 73, f. 25a-c. 
 
 “3 Nicholson and Eth. fil., Ann. and Mag. Nat. Hist., 1886, xvii., p. 181. 
 
 Sp. Char, Corallum ramose, dividing at wide intervals, the branches cylindrical, 
 averaging about two lines in diameter, and gradually tapering to their free extremities. 
 The corallites are nearly vertical in the axial portion of their course, but ultimately 
 bend outwards nearly at right angles to the imaginary axis of the branches, and 
 open on the surface by rounded calices which are free from any obliquity. As the 
 terminations of the branches are approached the angle of deflection of the corallites 
 becomes less and less, and the horizontal portion becomes shorter and shorter, until 
 at the extremity the whole of the corallites are nearly vertical. Average diameter 
 of the corallites from 7; to 25 inch, smaller tubes being intercalated among those of 
 average size as the surface is approached. Annular thickenings of the horizontal 
 portions of the tubes narrow and ring-like, about five occupying one line, this being 
 the total length, in general, of the annulated portions of the corallites. Surface not 
 observed. 
 
 Obs. This is a graceful and well-marked species, easily distinguished from 
 S. ovata and 8. tasmaniensis of Lonsdale by its habit and general proportions. We 
 should have been inclined to refer it to Stenopora (Chetetes) gracilis, Dana, which it 
 very closely resembles outwardly, had it not been for the fact that Dana lays stress upon 
 the length of the tubes in the latter species, as well as upon the remarkable paucity of 
 annulations in the same. 
 
 In the present species, on the other hand, the annulations of the tubes, in the 
 horizontal portions of their course, are much more numerous than in S. tasmaniensis, 
 Lonsd., while it differs conspicuously from 8. ovata, Lonsd., and other species, in its 
 size and general proportions. The presence of minute, irregularly placed mural pores 
 was formerly believed to be readily made out in specimens which are longitudinally 
 fractured, by an examination of the exterior of the tubes under low powers of the 
 microscope. A study of additional specimens, however, in the Mining and Geological 
 Museum, renders this point exceedingly doubtful, and it is more than probable that 
 they do not exist. 
 
 The corallum of 9S. Jackii is from three to six millimetres wide, the latter just 
 previous to bifurcation. Two tubes occupy the space of one millimetre, when seen in 
 longitudinal section. The mode of growth seems to be very regular and characteristic 
 in 8. Jackii, the corallum bifureating at wide intervals, and retaining a uniform thickness 
 throughout, until quite near the apices of the branches, when it tapers off to a 
 comparatively fine termination (PI. 6, fig. 11). 
 
 Loc. and Horizon. Coral Creck, Bowen River (&. LZ. Jack)—Middle or Marine 
 Series, Bowen River Coal Field. 
 
 It will be more convenient to describe herea Coral having many points in common 
 with S. Jackii, but differing in one or two very important particulars. This is repre- 
 sented in our Pl. 7, figs. 3, 4, 5. The mode of growth is the same, repeated simple 
 bifurcation at long intervals; the size of the corallum almost identical, from three to 
 five millimetres in width; whilst two tubes similarly occupy the space of one millimetre. 
 There is, however, this fundamental difference, that in this coral the tubes, although 
 much thickened, are simple and apparently non-annulate. Since the figures were drawn 
 I have had some excellent sections prepared, which demonstrate this feature in a very 
 decided manner, and I hope in a Supplement to this Work to illustrate this form much 
 more fully. 
 
206 
 
 The dendroid corallum was evidently of some size, as a specimen has been 
 observed three inches in length. The corallites radiate from an imaginary axis, and are 
 thin-walled in the axial region, but very much thickened in the peripheral zone, which is 
 short, and nearly at right angles to the former. The calices are round, or at times have 
 a tendency to become oval. The thickening of the walls is very uniform and regular, 
 the primordial wall occasionally being visible as an indistinct thin white line. String- 
 like thickenings in the walls have not been observed, but this feature very much depends 
 on preservation; whilst acanthopores are visible in a tangential section, irregularly 
 distributed, and each with a central papilla. The structure of the walls is, as usual in 
 these corals, laminar, the lamine directed convexly upwards. There are no pores, and 
 tabule have not been observed. 
 
 So well do the respective measurements of §. Jackii and the present coral agree, 
 that I should have unhesitatingly referred the latter to the former had it not been for 
 the total absence of tubular constrictiuns in this species. The differences observable in 
 the figures of the two forms are more apparent than real. 
 
 At present my investigations lave not satisfactorily demonstrated to what section 
 of the larger genus Monticulipora this fossil should be referred; but, without entering 
 into the question of the value of Orbdipora as a genus, as lately defined by Messrs. 
 Waagen and Wentzel,* the latter would seem to be a fitting temporary resting-place.f 
 As its provisional distinctness from 8. Jackii seems warranted by the structure, so far 
 as at present known, a name is desirable, and I would provisionally propose to call it 
 Orbipora? Waageni, as a slight appreciation of the valuable services rendered to 
 Paleontology by Dr. W. Waagen, late of the Indian Geological Survey. 
 
 Loc. and Horizon. Kooingal, near Gladstone (Lhe late James Smith) —Gympie 
 Beds. 
 
 STENOPORA GIMPIENSIS, sp. nov., Pl. 6, figs. 14 and 15. 
 
 Stenopora ? sp., Nicholson and Eth. fil., Ann. and Mag. Nat. Hist., 1879, iv., p. 276. 
 
 Sp. Char. Corallum ramose, the branches from two to five lines in diameter, 
 diverging from a main stem obliquely, or at right angles, the terminal portions always 
 bifureating, and the apices of the branches rounded or lobate. The corallites, after a 
 short vertical course in the axis of the branches, are abruptly deflected nearly at right 
 angles; and after holding this latter course for a space of from half a line to a line or 
 more, they open by direct apertures upon the surface. They are narrow but very 
 constant in size; walls very uniformly and regularly thickened, the thickening 
 increasing in amount as the calices are approached; structure is almost entirely 
 destroyed, but the primordial wall is visible at times as a thin broken line; moniliform 
 constrictions only visible in weathered specimens, the tubes always exhibiting in 
 fractured specimens a very delicately and minutely wrinkled appearance. Acantho- 
 pores large, but obscure, irregularly arranged, and at times surrounding the cealices. 
 Tabule present in the peripheral zone, although very much scattered, and rare, 
 horizontal. No pores visible. 
 
 Obs. This coral was originally referred to Stenopora, by Professor Nicholson 
 and the Writer, from general appearance only. We observed that though the coralla 
 are calcareous, and are themselves permeated by crystalline calcite, their more delicate 
 structures seem to have been destroyed during the process of fossilization, and micro- 
 scopic sections fail to show the internal structure in a thoroughly satisfactory manner. 
 
 
 
 
 
 * Pal. Indica (Salt Range Fossils), 1886, Ser. xiii., Vol. i., Pt. 6, p. 877. 
 + See Nicholson on the subject of the generic value of Orbipora. Genus Monticulipora and its Sub 
 Genera, 1881, pp. 11 and 24. 
 

 
 207 
 
 It was observed that the exterior of the tubes, in fractured specimens, was invariably 
 delicately wrinkled in the peripheral regions; but the fortunate occurrence of a 
 weathered and semi-decomposed specimen in Mr. De Vis’ Collection, revealed the 
 presence of very fine and regular moniliform constrictions of the genus. These do not 
 seem to be visible in any other state, and are certainly not to be seen in thin sections, 
 so far as our united observation has gone. 
 
 The corallum is usually from five to six millimetres wide, two tubes in the 
 peripheral region occupying the space of one millimetre. The bifurcation is very 
 regular, the branches always terminating in a lobato, or semi-plumose expansion. They 
 possess this character to a much larger extent than any other Stenopore, and the 
 individual branches are shorter. Herein lies a marked difference to Dana’s illustration 
 of his Stenopora (Chetetes) gracilis,* and an equally strong resemblance to his figure 
 of Stenopora ovata, Lonsdale.+ 
 
 The axial portion of the corallum is as correspondingly narrow, as the peripheral 
 is wide, and the angle of deflection between the two is a most marked one, quite a right 
 angle, the peripheral portion of the tubes being perfectly horizontal. 
 
 When compared with Stenopora Jackii the present species, S. gimpiensis, appears 
 more robust, with stronger branches, and in place of the regular annulations, the 
 exterior of the tubes is but faintly wrinkled. The stability of character displayed by 
 this coral marks it as a good species, which I propose to call Stenopora gimpiensis, from 
 its frequent occurrence in the rocks of that Goldfield. The figures (PI. 6, figs. 14 and 
 15) are not eminently satisfactory, and it will be refigured in the Supplement to this 
 Work. 
 
 Loc. and Horizon. Gympie, very characteristic of the green chloritic rock of 
 the Goldfield (The late R. Daintree, Colln. Brit. Mus.; &. L. Jack; C. W. De Vis, 
 Colln. Queensland Museum), 
 
 Sub-Kingdom—ECHINODERMATA. 
 Section—PELMATOZOA. 
 
 Obs. The remains of this division, with the exception of stem-joints, being of rare 
 occurrence in the Paleozoic rocks of Queensland, and usually very fragmentary, it has 
 been thought better to reproduce the whole hitherto collected, with the view of further 
 identification in the future. 
 
 Class—CRINOIDEA. 
 Order—COADUNATA, 
 Family—ACTINOCRINIDZ. 
 
 Genus—A CTINOCRINUS, Miller, 1821. 
 (Nat. Hist. Crinoidea, p. 90.) 
 
 
 
 ACTINOCRINUS, sp. znd., Pl. 7, fig. 9. 
 
 Obs. A cast of a few fragmentary plates, ornamented with tubercules and 
 radiating ridges, is referred to this genus. A more complete, although not so well 
 preserved specimen has been found by Mr. C. W. De Vis, in the neighbourhood of 
 
 * Geology Wilkes’ U.S, Explor. Exped., Atlas, t. 11, f. 10. 
 Telus ter lls fs 
 
208 
 
 Rockhampton, with similarly ornamented plates. The calyx has been obliquely pressed 
 to one side, and although obscure, the shallow basal cup and the succeeding radials can 
 be fairly made out. 
 
 Loc. and Horizon. Corner Creek, Great Star River (R. L. Jack)—Star Beds ; 
 Rockhampton District * (C. W. De Vis)—Gympie Beds. 
 
 Family—PLATYCRINIDZ. 
 
 Genus—PLATYCRINUS, Miller, 1821. 
 (Nat. Hist. Crinoidea, p. 73.) 
 
 PLATYCRINUS P NUX, sp. nov., Pl. 38, fig. 3. 
 
 Sp. Char. Calyx nut-shaped, length twenty-two millimetres, breadth fifteen 
 millimetres. Basal plates forming a well pronounced, moderately deep cup, to some 
 extent flattened on its articular or dorsal side ; articular facet for stem-joint small. Radial 
 plates oblong, gently convex, and straight-sided. The basals bear vertical, continuous, 
 well-separated ridges, which are continued on the radials, and are most conspicuous 
 on the distal two-thirds of the plates, where they spring from the basi-radial sutures 
 especially. 
 
 Obs. The foregoing are the only facts which can be gained from this imperfect 
 fossil, which appears to be an internal cast of the calyx. The long straight-sided 
 radials are very apparent, and, with a rather similar basal cup, give to the calyx a nut- 
 shaped outline, more particularly that of the hazel-nut. No other plates are preserved. 
 It is provisionally referred to Platycrinus rather than Dichocrinus, to which it also bears 
 some resemblance, but it must be admitted there is no trace of the articular margins 
 along the ventral edges of the radials. 
 
 Loe. and Horizon. Richards’ Homestead, three miles south-west of Mount 
 Britton Township, Lat. 8. 21° 20’, Long. E. 148° 30’ (A. Z. Morisset)—Middle or Marine 
 Series of the Bowen River Coal Field. 
 
 Order—INADUNATA, 
 Family—POTERIOCRINIDA. 
 
 Basat-Cur or Crrnorp, Pl. 44, fig. 7. 
 
 Obs. At first sight, this little cup has much the appearance of a Platycrinite, 
 but is perhaps made properly referable to one of the Encrinus-like genera with a 
 depressed or saucer-shaped calyx, such as Ceriocrinus, White, Hrisocrinus, M. & W., or 
 Stemmatocrinus, Trautschold. These are all Carboniferous genera, and mostly of rather 
 late date in that formation. 
 
 The under-basals in our little specimen form a flat dise, pentagonal in outline, 
 and apparently undivided. The basals seem to be pentagonal, and are, certainly, 
 abruptly bent upward, ‘the lower portion included in the truncate surface, the upper 
 almost vertical.’ These characters so strictly accord with those of Stemmatocrinus, that 
 it is better to provisionally include this fragment in that genus. 
 
 Loc. and Horizon. Rockhampton District * (C. W. De Vis)—Gympie Beds. 
 
 
 
 * See note, page 199, 
 
209 
 
 Genus—POTERIOCRINUS, Miller, 1821. 
 (Nat. Hist. Crinoidea, p. 67.) 
 
 Potertocrinus? Smrruit, sp. nov., Pl. 8, fig. 1. 
 
 Sp. Char. Culyx five millimetres high up to the articulation of the second radials, 
 and marked by strong longitudinal ridges, of which two are radial in position, and two 
 interradial ; the latter fork about the middle of the calyx, and the two branches of the 
 fork are continued right and left to the articular facets on the radials. From these 
 parts, therefore, three ridges proceed downwards, a radial one, and the right and left 
 branch, respectively, of the interradial ridges on either side of it. The position of the 
 basi-radial sutures is very obscure, but there seem to be indications of them at a 
 comparatively short distance from the upper edge of the calyx, so that the radial plates 
 would be relatively short, and the base high. The second radials, are short, transverse, 
 and oblong, but not as wide as the first radials; the third radials, or axillaries, are a 
 trifle longer, and pentagonal in shape, each bearing three arms; the outer remains 
 undivided, but the inner one consists of two joints (or first and second distichals), the 
 second of which is axillary, and bears two arms; the latter are composed of relatively 
 long and rounded quadrangular joints, with delicate pinnules. The stem consists of 
 numerous discoid joints, three or four of which are larger than the others, and bear 
 whorls of cirri. 
 
 Obs. This very interesting Crinoid is represented only by an impression on the 
 surface of a piece of hard sandstone, and from which casts have been taken. The base 
 is possibly dicyclic, but on this point the cast affords no definite information. The stem, 
 so far as preserved, is long, and there are thirty-five internodal joints below the two 
 lowest whorls of cirri, and about twenty in the next internode above. 
 
 The rather obscure state of preservation renders the reference of this Crinoid to 
 Poteriocrinus open to doubt; it is, however, believed to belong to that genus. Many 
 species of the latter appear to have whorls of cirri on the stem joints, especially near the 
 top of the stem. The same is the case in Hystricrinus, Hinde, some species of 
 Belemnocrinus, and a few other types. The only Neocrinoids with whorls of five cirri 
 are the Pentacrinide. 
 
 I have much pleasure in associating with this interesting species* the name of 
 the late Mr. James Smith, of Rockhampton, who was instrumental in bringing to light 
 many new fossils from that district. 
 
 Loc. and Horizon. Stanwell, near Rockhampton (Lhe late James Smith)— 
 Gympie Beds. 
 
 PorERIOCRINUS CRASSUS, Willer, Pl. 7, fig. 6. 
 
 Poteriocrinus crassus, Miller, Nat. Hist. Crinoidea, 1821, p. 68, plate. 
 . . T. and T. Austin, Mon. Recent and Foss. Crinoidea, 1848, p. 69, t. 8, f. 3a-m, t. 9, f. 1. 
 a By De Koninck and Lehon, Mém. Acad. R. Belgique, 1854, Mém. 8, p. 97, t. 1, f. 10a-d. 
 Obs. Numerous impressions of stems, quite indistinguishable from those of this 
 characteristic European Carboniferous species, were obtained by the late Mr. James 
 Smith, associated with Fenestella and Protoretepora. 
 One specimen represents a portion of a stem, eight inches long, with a large 
 number of strong cirri given off at close intervals. 
 Impressions of Crinoid stems appear to be very common in the Fenestella Beds 
 
 around Stanwell, in all stages of preservation, and many good examples were collected by 
 Mr. Smith. 
 
 * T am indebted for several suggestions on this species to the late Dr, P. H. Carpenter, F,R.S, 
 oO 
 
210 
 
 Loc. and Homzon. Encrinite Creek and Fenestella Hill, Stanwell, near Rock- 
 hampton (The late James Smith)—Gympie Beds. 
 
 In addition to those just described, the following specimens have been collected, 
 but are too imperfect to be definitely named :— 
 
 Arms or Crinorp, Pl. 7, fig. 7. 
 
 Obs. We have here the impressions of eight arms, or portions thereof, in their 
 present condition covered with pores or small pits. These represent blunt spines or 
 tubercles ornamenting the arm joints, such as are very well defined in some recent 
 forms. 
 
 Loc. and Horizon. Stanwell, near Rockhampton (The late James Smith; Colln. 
 Smith)—Gympie Beds. 
 
 Arms oF Crinorp, Pl. 7, fig. 8. 
 
 Obs. In this specimen may be seen the remains of nine or ten arms of another 
 Crinoid, In the centre is an axillary radial plate supporting two sets of five distichals, 
 followed by two pentagonal plates as axillary distichals, giving support to two series of 
 palmars. This succession is repeated in the series of plates on each side. This fossil 
 may belong to one of the Ichthyocrinide. 
 
 Loc. and Herizon. Stony Creek, Stanwell, near Rockhampton (The late James 
 Smith) —Gympie Beds. 
 
 Impresston OF Crrnorp Caryx, Pl. 44, fig. 8. 
 
 Obs. Pl. 44, fig. 8, represents a relief taken from an impression, on altered 
 shale, of a portion of a Crinoid calyx, with the bases of small arms. Little or no trace 
 of plates remain, but in the original the impression of the top stem-joint is visible. The 
 late Dr. P. H. Carpenter, to whom a reproduction was sent, was disposed to refer it to the 
 Platycrinide, from the above inequality in the plates and arms, amongst other characters. 
 
 Loc. and Horizon. Rockhampton District * (C. W. De Vis)—Gympie Beds. 
 
 CoLuUMNS. 
 
 The remains of Crinoid stems have been obtained by Mr. W. Leigh, at Spring- 
 sure, Central Railway; and by the late Mr. James Smith, plentifully, at Stony Creek, 
 Stanwell, and at Kooingal. In the Athelstane Range, Rockhampton, the latter Collector 
 found the remains of stems and corals, in an undeterminable condition, however, in a 
 very peculiar oolitic and brecciated rock, containing grains of quartz, calespar, felspar, 
 &c., cemented by a calcareous base, and decomposing into a spongy, friable mass. 
 
 Class—BLASTOIDEA. : 
 
 Order—REGULARES.t+ 
 Family—PENTREMITID~. 
 Genus—MESOBLASTUS, Eth. fil. and Carpenter, 1886. 
 (Cat. Blastoidea Brit. Mus., p. 181.) 
 MESOBLASTUS P AUSTRALIS, Etheridge jil., Pl. 44, fig. 2. 
 
 Sp. Char. Calyx bi-pyramidal, tapering to both extremities; summit and base 
 both small and narrow; periphery at the radio-deltoid suture. Basal plates forming a 
 
 
 
 * See note, p. 199. 
 + Etheridge fil. and Carpenter—Catalogue of the Blastoidea in the Geological Department of the 
 
 British Museum (Nat, Hist,), 1886, p, 148, 
 
211 
 
 small conical cup. Radial plates oblong, and apparently spreading; bodies and limbs 
 of nearly equal length. Sinuses long, narrow, parallel-sided, and nearly equally 
 excavated between the radial and deltoid plates in two planes, the proximal or longer 
 sloping away to the summit, the lower or distal directed towards the base, and shortest 
 of the two. Radio-deltoid sutures strongly V-shaped. The deltoid plates are large, 
 sharply lanceolate, and their surfaces probably a little concave. Ambulacra very long, 
 narrow, parallel-sided ; lancet plates slightly exposed; side plates small, at least forty 
 on each side, ambulacral. grooves rather deep, and much crenulated. Spiracles, 
 hydrospires, and mouth unknown. Sculpture of radial and deltoid plates parallel to 
 their outlines; that of the former consisting of ridges, separated by corresponding 
 depressions ; but on the latter the V-shaped lines become sub-imbricate. 
 
 Obs. I am constrained to place this anomalous form provisionally in 
 Mesoblastus, although sensible that this is far from being its correct resting place. 
 The general outline, contracted summit, and covered lancet plates, separate it at once 
 from Pentremites, as that genus is now understood. The same characters indicate 
 Pentremitidea as a near ally, but the large lanceolate deltoid plates quite forbid such 
 areference. The only other genus of the family Pentremitide, the family to which the 
 Blastoid clearly belongs, is Mesoblastus, E. and C. The resemblance between this genus 
 and our species is so far identical that, in both, the deltoids are visible in a side view 
 and conspicuous, the ambulacra narrow, without being linear in the sense as in the genus 
 Metablastus, and there is to some slight extent a resemblance in form. In other 
 features, on the other hand, IZ. ? australis does not conform to the structure of 
 Mesoblastus, and it is possible that a new genus will be required for its reception. I 
 am, however, not prepared to deny that it may not be an abnormal Mesoblastus, with 
 both deltoids and base rather larger than usual in species of the latter. 
 
 A very peculiar feature is exhibited by this specimen, which, if real, and not 
 superinduced by distortion or crushing, will separate it from all known Blastoids. At 
 the radio-deltoid sutures the two neice ambulacra are bent down at a sharp angle, 
 following the bi-pyramidal outline of the calyx. From the appearance of certain 
 markings I was led at first to regard this as the result of fracture, but the bilateral 
 symmetry, and undistorted state of the calyx would appear to indicate otherwise. To 
 restore these ambulacra to the evenly convex outline found in Blastoids, in which the 
 ambulacra extend beyond the periphery, would so disarrange the radial plates as to 
 remove all semblance in the specimen to a Blastoid at all. I am therefore constrained 
 to regard this angulation of the ambulacra as, to some extent, a feature of the species. 
 This curvature is met with in several genera, Jesoblastus, Schizoblastus, and especially 
 Granatocrinus, but not to such an extreme extent as in the present species. 
 
 I shall look forward with interest to the acquisition of further specimens, with the 
 view of ascertaining how far this explanation of its structure holds good in ML. ? australis. 
 
 Loc. and Horizon. Rockhampton District * (0. W. De Vis)—Gympie Beds. 
 
 Family—GRANATOBLASTID + 
 
 Genus—GRANATOCRINUS, Troost, 1849. 
 Cioer: Jour. Sci., viil., p. 420; Emend., Etheridge fil. and Carpenter, Catologue, loc. cit., p. 288.) 
 GRANATOCRINUS ? WACHSMUTHII, sp. nov., Pl. 7, fig. 10. 
 
 Obs. Under this name is figured the first discovered remains of an Australian 
 Blastoid, and it affords me great pleasure to associate it with the name of Mr. Chas. 
 
 
 
 
 
 * See note, p. 199. 
 + Etheridge fil. and Carpenter, Catalogue, Joc. cit., p. 287. 
 
212 
 
 Wachsmuth, of Burlington, Towa, to whom J was, in former years, in company with 
 the late Dr. P. H. Carpenter, ; Prontly indebted for very kind and exceptional assistance 
 when working out the structure of the Blastoidea. 
 
 The specimen is only the partial impression of a calyx on a piece of indurated 
 shale, but is still sufficient to show how distinct it is from either of the other Australian 
 Blastoids. Anambulacrum is visible, containing a large number of plates, and highly 
 ornate bounding plates. But whether these are radials, or large deltoids, after the type 
 of Granatocrinus derbiensis, G. B. Sby.,* it is difficult to say on account of the state of 
 preservation, but probably the latter will be the correct reading. The summit seems to 
 have been moderately large and truncate. Apparently a good deal of lateral pressure 
 has taken place, otherwise it is difficult to account for the position and function of the 
 large elongated plate immediately on the left (Pl. 7, fig. 10) of the radial sinus in the 
 figure. 
 
 Loe. and Horizon. Stanwell, near Rockhampton (The late James Smith)—Gympie 
 Beds. 
 
 Family—TROOSTOBLASTIDZ.+ 
 
 Genus—TRICHLOCRINUS, Meek § Worthen, 1868. 
 (Proc, Acad. Nat. Sci. Philad., p. 356.) 
 
 TRICHLOCRINUS ? CARPENTERT,{ sp. nov., Pl. 44, fig. 3 
 
 Sp. Char. Calyx large, elongately barrel-shaped, or ovate, bi-pyramidal, attenu- 
 ated both dorsally and ventrally ; summit less contracted than is usual in this genus; 
 base rather long, the excavations along the lines of the interbasal sutures wide and 
 shallow, and extending as far as the radio-deltoid sutures; proximal or ventral section 
 probably oval, or almost round, with rather rounded sides; distal or dorsal section 
 indefinitely pentagonal, but more regularly so along a line drawn through the radial lips. 
 Radial plates large, long, the lateral margins diverging, and giving an expanded appear- 
 ance to the plates; bodies more than half*the length of the limbs, moderately carinate ; 
 limbs narrowing upwards, their proximal margins very oblique; interradial sutures 
 straight, in shallow concavities; radio-deltoid sutures deeply V-shaped, each half straight, 
 sinuses long, narrow, and parallel-sided ; radial lips but little marked. Deltoid plates | 
 large, elongately and unequally rhombic, more than one-third as long as the calyx. 
 Ambulacra very narrow and of uniform width the distal fourth not penetrating each 
 radial plate ; lancet plate long, narrow, and but very gradually tapering ; hydrospires 
 four on each side, pendent for three-fourths the length of the ambulacra, and probably 
 retained within the substance of the radials for the remaining distal fourth. 
 
 Obs. The test, basal plates, mouth, and spiracles are not preserved. Although 
 retaining all the general characters of Tricelocrinus but one, the calyx is much more 
 oval and barrel-shaped than any described species of this peculiar genus. It departs 
 entirely from the usual type in ‘the possession of very large Bbnk ; but as those of 
 T. obliquatus, Roemer, are not known, and those of 7. Meekianus show an advance in 
 size on the similar plates in the type species, 7. Woodmant, I have determined for the 
 
 
 
 * Etheridge fil. and Carpenter, Catalogue, Joc. cit., t. 9, f. 1 and 2. 
 
 + Etheridge fil. and Carpenter, Catalogue, loc. cit., p. 190. 
 
 + The Writer desires to place on record his mite of testimony to the great loss Biology has sustained in 
 the early and untimely death of his excellent Friend and Co-writer, Phillip Herbert Carpenter, D.Sc., F.R.S. 
 No one amongst the latter’s circle of acquaintance was probably in a better position to estimate the manly, 
 upright, unselfish, and truthfully honest career of P. H. Carpenter than was the Writer, from his close 
 association with him for many years in scientific work, and no one has certainly felt his decease more. 
 (R, £. Junr.) 
 
SS — OT 
 
 —————————— 
 
 213 
 
 present to retain this species in the present genus. So far as its specific position 1s 
 concerned it is unquestionably a new form. The large deltoids, and the fact of the 
 radial sinuses being so largely enclosed by those plates, as well as the shallow basal 
 excavations along the lines of the interradial sutures, are points of.the highest 
 importance. 
 
 The structure of the ambulacra resembles that seen in 7. obliquatus, Roemer. 
 A little below the intersection of the sinuses by the radio-deltoid sutures, the impres- 
 sions of the ambulacra on the surface of the cast abruptly cease. From these points, 
 arguing by analogy, it is more than probable that they become enclosed within the 
 substance of the radial plates. The surface of the cast below the visible terminations 
 of the ambulacra is flattened and harpoon-head shaped, the apices representing the 
 radial lips. At the proximal end of this depression are visible four hydrospire-sacs on 
 each side, the outer ones becoming so much curved as to be almost at right angles to 
 the ambulacra. The structure of this part of the economy of TZ. Carpenteri would 
 seem to show that the hydrospires beneath the calyx plates were not cut off from the 
 body cavity to the same extent as surmised by the late Dr. P. H. Carpenter and the 
 Writer when describing the genus generally.* A comparison with our figures ¢ of the 
 interior and exterior of the radial plates of 7. obliquatus will fully demonstrate the point. 
 This, no doubt, arises from the much greater development of the deltoid plates in the 
 Australian species at the expense of the radials. 
 
 Structural details of the spiracles in Tricwlocrinus are much needed, and I 
 regret that the otherwise instructive cast now before me does not directly so assist. 
 But I believe the hydrospire canals are visible in one of the interradial areas, and 
 partly so in a second. Their: structure is not altogether clear, but it seems to be 
 generally in accordance with that scen in the class. 
 
 Loc. and Horizon. Rockhampton District t (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 Section—ECHINOZOA. 
 Class—ECHINOIDEA. 
 
 Order—PALECHINOIDEA. 
 Family—A RCH AOCIDARID A. 
 
 Genus—ARCHGCIDARIS, McCoy, 1884. 
 (Synop. Carb. Limest. Foss. Ireland, p. 173.) 
 
 Obs. The only evidence of the existence of this important group in the 
 Paleozoic rocks of Queensland is the occurrence of a single plate, or rather the 
 impression of it, in Mr. De Vis’ Collection. The impression is, as usual, hexagonal, the 
 margins granular, and the surface between the latter and the central tubercle flat. The 
 latter is strong and well marked. It is certainly an interambulacral plate of a member 
 of this family, and probably of the type genus. I believe this to be the first announce- 
 ment of the occurrence of the Palechinoidea in Australian Permo-Carboniferous 
 rocks. 
 
 Loc. and Horizon. Rockhampton District t (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 * Catalogue, loc. cit., p. 205. 
 + Ibid., t. 18, f. 10-13. 
 + See note, page 199, 
 
214 
 
 Sub-Kingdom—ANNULOSA. 
 Class—CRUSTACEA. 
 Order—OSTRACODA., 
 
 Family —LEPERDITID&. 
 
 Genus—BEYRICHTA, McCoy, 1846. 
 (Sil. Foss. Ireland, 1846, p. 57.) 
 
 Bryricuta varicosa, 7. R. Jones, sp. nov., Pl. 7, fig. 15. 
 
 Obs. ‘*An internal cast of a right valve showing three main lobes as in B. 
 Kledeni, but with differences. Thus the central lobe is nearly isolated: the two outer 
 lobes are continuous below, and the hinder lobe is partially intersected from the dorsal 
 edge, so that a small but definite supernumerary lobe is almost divided off from its inner 
 (medial) ridge. The valve had a strongly flanged lip on its free margin, non-represented 
 by a deep sloping furrow, stronger behind than in front. The dorsal and partly the 
 anterior edge of the cast are obscured with matrix. Length of the valve two millimetres, 
 height one millimetre.” 
 
 On submitting this pretty little Beyrichia to Prof. T. R. Jones, F.R.S., he was 
 kind enough to favour me with the above observations. He believes it to be 
 distinct from any species of Beyricha hitherto published, and it forms a welcome 
 addition to the scanty Ostracod fauna, hitherto described from the Upper Palzozoie 
 rocks of Australia. 
 
 Loc. and Horizon. Corner Creek, Great Star River (R&R. LZ. Jack)—Star 
 Beds. 
 
 Order—TRILOBITA. 
 Family—PR@TIDZ. 
 
 Genus—PHILLIPSTIA, Portlock, 1843. 
 (Report Geol. Londonderry, Tyrone, &c., p. 305.) 
 
 PHILLIPSIA DUBIA, Htheridge, sp. 
 
 Pl. 7, fig. 12; Pl. 8, figs. 5 and 6; Pl. 44, fig 4. 
 
 Grifithides dubius, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 338, t. 18, f. 7. 
 
 Sp. Char. Body ovate-oblong, length about twice the width, sides parallel; 
 general axis equal in width to the pleure ; cephalic shield and pygidium about equal in 
 length, but somewhat shorter than the body respectively. Cephalic shield semi-circular, 
 with rounded genal angles, anterior border striate; glabella ovate pyriform,and narrowing 
 towards the front, gently convex anteriorly, but rather flattened behind, not in any way 
 overhanging the anterior edge of the shield ; basal lobes prominent, rounded, and pea- 
 like, deeply cut off by the neck furrow; basal furrows well marked, but the ocular 
 furrows faint, oblique, and short, and the frontal furrows invisible ; palpebral lobes but 
 faintly developed, and narrow; free cheeks elongately triangular, with nearly vertical 
 and delicately striate surrounding rim; eyes moderately long, and rather narrow, but 
 most minutely facetted; neck furrow behind the glabella broad and deep. Thoracic 
 
215 
 
 segments nine to ten; axis very distinct, and as wide as the pleura, with strong axial 
 furrows; pleure much bent down, with wide and spathulate facets. Pygidium of ten 
 segments, without any terminal spine; margin entire, nearly vertical, and striate ; 
 furrows of limbs wide and shallow. Testaceous sculpture unknown. 
 
 Obs. The above description is taken from a very perfect individual, collected by 
 Mr. P. W. Pears, from which the test had been removed. The presence of the shelly 
 matter would only modify the above expressions in but a slight degree. 
 
 The presence of the glabella furrows at once removes this species from 
 Grifithides, and indicates Phillipsia as its proper resting place. It even appears to be 
 peculiar amongst the species of this genus, for the remarkable diminution in width of 
 the glabella forwards. Mr. Rk. Etheridge, F.R.S., described P. dubia as possessing from 
 ten to twelve thoracic segments, but there appear to be only ten at the outside in the 
 present specimen. 
 
 Toc. and Horizon. Don River, Queensland* (The late R. Daintree)—Gympie 
 Beds; Corner Creek, Great Star River (R. LZ. Jack and P. W. Pears)—Star 
 Beds. 
 
 Puivirps1a WOODWARDI, sp. nov. 
 Pl. 7, figs. 11 and 13; PI. 8, fig. 6; Pl. 44, figs. 5 and 6. 
 
 Sp. Char. Glabella round, without any lateral inflection of the margin, 
 moderately convex in the middle line, and a little arched posteriorly ; neck furrow 
 strong and deep, with more or less complete basal furrows; anterior furrows present, 
 but faint ; anterior border thick and upwardly turned, leaving a wide depression between 
 it and the front of the glabella. 
 
 Obs. This is a much larger and rounder form than P. dubia; but the marked 
 feature is the upwardly turned front rim to the head, separated from the front of the 
 glabella, a character sometimes met with in this genus, but not often, as the border is 
 usually confined to the immediate front edge of the glabella. In general appearance 
 P. Woodwardi resembles some species of the allied genus Pretus, and in its remarkable 
 rotundity Cheirurus. 
 
 The glabella of P. Woodwardi may be distinguished from that of P. dubia by its 
 continuous and non-indented outline. 
 
 The pygidium referred to is much larger than that described as P. dubia, but 
 otherwise resembles it ; and again only differs from the Trilobite figured by Dr. Koninck 
 as Griffithides Hichwaldi in having a rather narrower axis; in fact it is quite possible 
 that the two may be identical. De Koninck’s reference of a New South Wales Trilobite 
 to that species is, I believe, erroneous. The pygidium he figures is much too round for 
 G. Hichwaldi, and not so long from before backwards, being more semi-circular and less 
 deltoid. 
 
 Loc. and Horizon. Stony Creek, Stanwell, near Rockhampton (The late James 
 Smith)—Gympie Beds. 
 
 PHILLIPSIA? sp. ind. 
 
 Obs. Portions of the largest Permo-Carboniferous Trilobite I have yet seen from 
 Australia were collected by the late Mr. James Smith, in the neighbourhood of Mount 
 Morgan. It is the half of a pygidium, measuring across the anterior end, from the 
 border of the pleura to the centre of the axis, exactly half-an-inch, giving one inch as 
 
 
 
 * The Don River referred to by Mr. Etheridge must be the tributary of the Dawson of that name— 
 (Lat. 24° S,, Long. 150° 20’ E.) It cannot be the Don River near Bowen. (R.Z.J.) 
 
216 
 
 the full width of the pygidium. The specimen is quite decorticated and without test. 
 There are fourteen to sixteen pleure visible, the anterior ones rather sigmoidal in 
 outline. The perfect tail was probably broad oval, or shield-shaped, and many of the 
 pleural grooves are wide and open. 
 
 This fossil is, in all probability, undescribed, and its imperfect eondioue is to be 
 regretted. If new, I would propose for it the name of Phillipsia ? grandis. It will be 
 figured in a separate Paper on Queensland fossils. 
 
 Loc. and Horizon. West of the Dividing Range, at the Crow’s Nest, near 
 Mount Victoria, near Mount Morgan (The late James Smith ; Mining and Geol. Mus., 
 
 Sydney)—Gympie Beds. 
 
 Genus—GRIFFITHIDES, Portlock, 1843. 
 (Geol. Report, Londonderry, &c., p. 310.) 
 
 GRIFFITHIDES SEMINIFERUS, Phillips, sp. ?, Pl. 7, fig. 14. 
 
 Asaphus seminiferus, Phillips, Ill. Geol. York, 1836, Pt. 2, p. 240, t. 22, f. 8-10. 
 Phillipsia seminifera, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 348, t. 24, f. 9 and 9a. 
 Griffithides seminiferus, Woodward, Mon. Brit. Carb. Trilobites, 1883, Pt. 1, p. 28, t. 28, f. 1-9. 
 
 Obs. <A Trilobite, in many features resembling this species, has been obtained at 
 two localities. At one it is represented only by a small free cheek (Pl. 17, fig. 14), but 
 possessing the same ornament, and generally resembling De Koninck’s figure, as above 
 given. The other specimens consist of portions of two individuals much displaced, but 
 clearly showing that from ten to eleven thoracic rings existed, very convex and rounded. 
 The glabella was short and semi-circular, broad and densely granuled, the basal lobes 
 large, and the lateral terminations of the pleure large and spathulate. The limb of the 
 glabella and pygidium was striate. 
 
 Although otherwise corresponding with G. seminiferus, the latter has the advantage 
 of size, and the limbs are plain. This, however, I opine, can hardly constitute a specific 
 difference, but it may perhaps render our form a good variety, and it may be known 
 as G. seminiferus, var. australasica, 
 
 Loc.and Horizon. Stony Creek, Stanwell (Lhe late James Smith); Rockhampton 
 District * (C. W. De Vis; Colln. De Vis)—Gympie Beds. 
 
 Sub-Kingdom—MOLLUSCA. 
 
 Class—PoLyYZOA. 
 
 Obs. The determination of fossils of this class found in the Upper Paleozoi¢ rocks 
 of Eastern Australia is rendered exceedingly difficult by their imperfect state of preser- 
 vation, found, as they usually are, merely in the condition of impressions. In such 
 specimens the whole of the substance of the polyzoarium has been removed, leaving 
 usually not the slightest trace of the cells, but is merely represented by the hollow 
 spaces from which the stems and branches have disappeared, and the cast of the mesh- 
 like fenestrules. - This state of preservation has rendered identification very difficult, a 
 difficulty not decreased by the obviously perplexing manner in which the characters of 
 the species appear to run into one another. In the absence of definite information 
 concerning the nature of the cells, it becomes very difficult to distinguish between 
 species, so little reliance can be placed upon the size and relative distance apart of the 
 meshes of the polyzoarium. 
 
 * See note, p. 199. 
 
217 
 
 Since my remarks on the Polyzoa of the Bowen River Coal Field were written ,* 
 I have succeeded in finding + the original specimens collected by the late Count P. de 
 Strzelecki, and figured by the late Prof. Morris in the work of the former, and am 
 therefore able to form a much better conception of the species. 
 
 Order—GYMNOLEMATA., 
 Sub-Order—CYCLOSTOMATA. 
 Family—FENESTELLID A. 
 Genus—FENESTELLA, Lonsdale, 1839. 
 
 (Murchison’s Silurian System, p. 677.) 
 
 FENESTELLA FossuLA, Lonsdale, Pl. 9, figs. 4 and 5. 
 Fenestella fossula, Lonsdale in Darwin’s Geol. Obs. Vole. Islands, 1844, p. 166. 
 
 ” 98 Lonsdale in Strzelecki’s Phys. Descrip. N. 8. Wales, &c., 1845, p. 269, t. 9, f. 1. 
 93 Ae Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii. Pt. 1, p. 332, t. 25, f. 1. 
 
 »,  plebeia (pars), Etheridge fil., Cat. Australian Foss., 1878, p 43. 
 ” sp. ind., Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 279. 
 
 Sp. Char. Polyzoarium infundibuliform, curled on the upper surface, structure 
 very regular. Interstices and dissepiments remarkably regular, fine, slender, or almost 
 hair-like, the former with a fine median keel, and branching dichotomously, but rarely. 
 Cells very small, increasing to three rows below each bifureation of an interstice, and 
 from three to four corresponding to each fenestrule in vertical series, one being 
 usually placed opposite the end of each dissepiment. Fenestrules square-oval. 
 Reverse face usually striate granular. 
 
 Obs. In the “ Catalogue of Australian Fossils”? I included F. fossula as a 
 synonym of F. plebeia, McCoy, chiefly in deference to the opinion of Prof. L. G. de 
 Koninck.{t After examining the Strzeleckian type in the National Collection, however, 
 I am unable to support this view, and believe that & fossula will prove distinct from 
 McCoy’s species. 
 
 The general appearance is quite different to that of / plebeta. It is reiatively 
 much smaller and finer, the interstices more closely packed together, giving rise to that 
 appearance which suggested to Mr. R. Etheridge, F.R.S., the name of F. densa.§ There 
 is a total absence of the erect, rigid, and wiry appearance so common to F. plebeia. 
 
 In describing F. fossula, Lonsdale distinetly says, ‘‘ Celluliferous face internal,” 
 and several exceedingly good specimens in the Mining and Geological Museum, Sydney, 
 show the curled and infundibuliform expansion to be so, and the branches only celluli- 
 ferous. The rows of zoecia vary from two to five, usually the former, but sometimes 
 three rows predominate. The increase, however, usually takes place on a branch about 
 to bifurcate, and the rows are invariably separated by keels or longitudinal dividing 
 ridges... Both this and the succeeding species quite lack the rigid, wiry look of 
 Polypora. 
 
 Fenestella jabiensis, Waagen and Pichl,|| from the Salt Range, is very closely 
 allied to this, judging from the fragments figured, but is perhaps of rather too large 
 a habit. 
 
 * Proc. R. Phys. Soc. Edinb., 1880, v., p. 273. 
 
 + In the Geological Department of the British Museum (Natural History), London. 
 tToss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 171. 
 
 § Quart. Journ. Geol. Soc., 1872, xxvili., p. 332. 
 
 || Pal. Indica (Salt Range Foss.), 1885, Ser. xiii., Pt. 1, No. 5, p. 778, t. 88, ff. la-d and 2. 
 
218 : 
 
 Loe and Horizon. Smithfield Reef, Gympie, and Blackfellows’ Diggings, Rock- 
 hampton (The late R Daintree; Colln. Geol. Surv., Queensland, and British 
 Museum)—Gympie Beds; Coral Creek, below Sonoma Road-crossing, and Stone- 
 humpy Creek, Bowen River (2. L. Jack)—Middle or Marine Series, Bowen River Coal 
 Field ; Lake’s Creek, near Rockhampton (Lhe late James Smith)—Gympie Beds. 
 
 FENESTELLA INTERNATA, Lonsdale, Pl. 9, figs. 6 and 7. 
 
 Fenestella internata, Lonsdale in Darwin’s Geol. Obs. Vole. Islands, 18-44, p. 165. 
 a . Lonsdale in Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 269, t. 9, ff. 2, 2a-e. 
 3 Dana in Geology Wilkes’ U. 8. Explor. Exped., 1849, p. 710, atlas, t. 10, f. 13-0. 
 
 Sp. Char. Polyzoarium infundibuliform, regular in appearance. Interstices 
 narrow, straight, medianly keeled and sometimes tuberculate, and frequently dichotomis- 
 ing; dissepiments short, of less breadth than the interstices. Fenestrules oval. Cells 
 round, three to a fenestrule, two being situated on each margin, and one opposite the 
 dissepiments on each side. Reverse granular-striate. 
 
 Obs. F. internata appears to differ from F. fossula only in being of a larger 
 habit, and although a regular closely knit species it does possess the same densely 
 retiform appearance. In the case of this species, Lonsdale again distinctly says that 
 the celluliferous face is internal. The examples from Queensland, like the type, are 
 casts only, or rather impressions left by the removal or decay of the polyzoarium. In 
 such instances it is exceedingly difficult, even with the aid of squeezes in relief, taken 
 from them, to express with accuracy the characters of the fossil under description. 
 When only two rows of zoecia exist on the branches of this species, the dividing keel is 
 straight and sharp; but when the latter is augmented they become less defined and 
 wavy. This is equally visible in Tasmanian specimens. 
 
 Loe. and Horizon. Fenestella Hill, Stanwell, near Rockhampton (The late 
 James Smith)—Gympie Beds. 
 
 FENESTELLA, sp. ind. 
 Fenestella, sp. ind., Etheridge fil., Trans. R. Soc. Vict,, 1876, xii., p. 68, pl., f. 2 and 2a. 
 
 Obs. This form bears a resemblance to Lonsdale’s F. internata, but it is 
 apparently too large in habit, and the number of cells in a given space is too great. It 
 was evidently a large and handsome species. The interstices are carinate, and the cells 
 from four to six within the length of a fenestrule; the latter appear to have been oval. 
 In places a third row of cells is developed, especially previous to the bifurcation of the 
 interstices. Only one specimen has been examined. 
 
 Loc. and Horizon. Gympie (The late R. Daintree; Colln. British Museum). 
 Fenestella has also been obtained at Kooingal (The late James Smith)—Gympie Beds. 
 
 FENESTELLA MULTIPORATA, De Koninck, Pl. 8, figs. 7 and 8. 
 
 Fenestella multiporata, De Koninck (non McCoy), Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 175, 
 ity toy tip die 
 
 Obs. A small and pretty Fenestella, corresponding with the F. multiporata of 
 De Koninck, but not of McCoy.* Both De Koninck’s illustration, and the present 
 specimen, although possessing the same number of cells to a fenestrule as McCoy’s 
 species, differ wholly from the latter in the small size and habit of the polyzoarium. 
 This is certainly the case as regards Prof. De Koninck’s figure, notwithstanding his 
 very positive assertions to the contrary. 
 
 
 
 * Synop. Carb. Limest. Foss. Ireland, 1844, p. 203. 
 
219 
 
 The identity of many of De Koninck’s species is rendered very difficult by the 
 careless mistakes which are made in the reference-numbers of the figures given in the 
 text, and in the Plate-Explanations. The present is a case in point—in the text 
 F. multiporata is said to be Pl. viii., fig. 4, when it should be fig. 1. | 
 
 The polyzoarium of this species would seem to have been fan-shaped, and 
 certainly its features are very minute and delicate. The length of the fenestrule will 
 at once distinguish it from F. fossula. 
 
 Loc. and Horizon. Corner Creek, Great Star River (RB. L. Jack)—Star Beds. 
 
 Genus—POLYPORA, McCoy, 1844. 
 (Synop. Carb. Limest. Foss. Ireland, p. 206.) 
 
 Potypora ? SMrrutt, sp. nov., Pl. 9, figs. 1-3; Pl. 44, figs. 9 and 10. 
 
 Sp. Char. Polyzoarium crumpled and curled, and probably infundibuliform, 
 composed of very straight, rigid, and regular interstices, bifurcating at long intervals, 
 and retaining the same width throughout. Dissepiments short, thin, and also very 
 regular. Fenestrules narrow, and long-oval. Cell-mouths arranged in three or four 
 oblique rows across the interstices. Reverse with very fine and regular longitudinal 
 striw, or occasionally granular striate. 
 
 Obs. A tendency to wide bifureation, accompanied by the erect habit, give to 
 this form a fan-like appearance, producing a very marked character. The several rows 
 of cell apertures on the interstices, and their absence on the dissepiments, appear to 
 indicate this as a species of Polypora. The fan-shaped polyzoarium is crumpled and 
 curled to some extent; but at present no satisfactory evidence can be adduced to show 
 that the poriferous face was internal, as in Protoretepora. It is provisionally, there- 
 fore, referred to Polypora. I have seen this interesting Polyzoon from two localities 
 in Queensland, but from one of them, Fenestella Hill, Stanwell, there are large fronds 
 of a somewhat smaller habit, which may be only a variety. 
 
 P. ? Smithit partakes of the habit of P. gigantea, Waagen and Pichl,* but is 
 decidedly smaller in all its parts; neither does it correspond to the close retiform or 
 Phyllopora-like species usually met with in the Carboniferous rocks of other areas. 
 P. ? Smithit will require further working out from additional and better preserved 
 material. 
 
 An impression (Pl. 44, figs. 9 and 10) of the poriferous face of a stiff-and 
 somewhat rigid form has been obtained at Gympie by Mr. W. H. Rands. The fenestrules 
 are long and narrow, the interstices erect, straight, and thin. The dissepiments are 
 small and short, whilst the cells vary from six to nine to a fenestrule, three alternating 
 rows on each interstice, with prominent exsert mouths. The obverse surface is 
 delicately striate. 
 
 Loc. and Horizon. Blackfellows’ Diggings, near Rockhampton (The late R. 
 Daintree; Colln. Brit. Mus.) ; Fenesteila Hill, Stanwell, near Rockhampton (The late 
 James Smith); Hill near Nos. 7 and 8, Lady Mary Reef, Gympie (W. H. Rands)— 
 Gympie Beds (PI. 44, figs. 9 and 10.) 
 
 Genus—PROTORETEPORA, De Koninck, 1877. 
 
 Protoretepora, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 178. 
 Etheridge fil., Proc. R. Phys. Soc. Edinb. 1880, v., p. 275. 
 
 Gen. Char. Polyzoarium infundibuliform, pedunculated, frequently of large 
 extent, forming either a simple funnel-shaped expansion, sometimes wavy along its 
 
 99 
 
 
 
 * Pal. Indica (Salt Range Foss.), 1885, Ser. xiii., Pt. 1, No. 5, t. 89, f. 1 and 2. 
 
220 
 
 upper margin, or one much crumpled, contorted, and curled. Dissepiments and 
 interstices but little differentiated (except by the much greater breadth of those 
 portions representing the former), more or less coalescent and the interstices many 
 times dichotomous. Fenestrules. numerous, oval or round, arranged in regular vertical 
 series. Celluliferous surface internal, the dissepiments usually cell-bearing. Basal 
 plate thin. Outer surface striate or granular. 
 
 Obs. The names Fenestella and Polypora had been indiscriminately used by 
 some Writers for colonies which really possess the characters of Phyllopora, except that 
 the cell-bearing face, or aspect of the polyzoarium, was internal instead of external, as 
 expressly stated by Professor W. King in the case of his genus. It is for these 
 
 -infundibuliform and intermediate Phyllopora-like forms that Professor L. G. De 
 Koninck has proposed his genus Protoretepora. In a few words it may be said to differ 
 from allied genera, as follows:—From Fenestella, by having the whole of one face of 
 the polyzoarium cell-bearing, and that the internal instead of either the internal or 
 external, and the cells not limited to the interstices only; from Polypora, by the 
 absence of a well-defined separation of the polyzoarium into interstices and dissepiments, 
 and the whole of the cell-bearing face celluliferous; lastly, from Phyllopora, simply 
 by the fact that the celluliferous aspect is internal, and not external, the arrange- 
 ment and disposition of the cells being exactly the same. 
 
 Protoretepora would at first sight appear to have close relations to the recent 
 Retepora, and it appears that the only reason assigned for their separation by Professor 
 De Koninck scarcely seems sufficient. He says that ‘in Metepora, properly speaking, 
 the branches are arranged (contournées) in such a way as to form meshes, and not regular 
 rows of ‘ oscules’ or fenestrules”’ (¢.e., as in Protoretepora). 
 
 After examining carefully a specimen of the recent Retepora Beaniana (King), 
 one cannot see that the difference pointed out by Prof. De Koninck is of sufficient 
 importance in itself to base a generic separation on. On the other hand, if we look a 
 little more minutely into the subject, we shall find a much more satisfactory reason for 
 the separation of the two forms. 
 
 Lonsdale long ago pointed out in describing * his Fenestella ampla, that the 
 polyzoarium was bilamellar, the outer layer or back of the branches being “ composed 
 of a uniform crust,” upon which are seated the tubular cells, at right angles, or a little 
 obliquely to the former. This structure is exceedingly well shown in Mr. Lonsdale’s 
 figure given in Count Strzelecki’s work, but we are indebted for a further and fuller 
 exposition of it to Professor W. King. This Author showed { that in his genus 
 Phyllopora, and some other Palsozoie genera, the frond was bilamellar or bistructural, 
 consisting of a lamina of capillary tubes, called the basal plate, and an outer lamina of 
 cellules, arranged more or less at right angles to, and on this. On the other hand, 
 he states that in the Elasmoporide (—Reteporide, Auct.), the frond is uni-lamello- 
 celluliferous, ‘composed of one lamina, consisting simply of cellules or polypidoms.” As. 
 before stated, this bilamellar structure has been shown to exist in Protoretepora ampla, 
 by Lonsdale, and it appears to me a character of much more generic value than the 
 mere arrangement of the fenestrules only. 
 
 The distinction between Fenestella and Protoretepora is even more than a generic 
 one, it is even that of a sub-family. In the former the cells are arranged in regular 
 rows on each side, a prominent keel traversing every branch. In the later genus the 
 
 
 
 * Darwin’s Geol. Obs, Vole. Islands, pp. 163, 164. 
 + Phys. Descrip. N. S. Wales, &c., 1845, t. 9, f. 3d. 
 + Ann. and Mag. Nat. Hist., 1849, pp, 388-90; Mon. Perm, Foss. England, 1852, p. 42, 
 
221 
 
 whole of the branch surfaces are celluliferous without any separation by ridges. The 
 separation of the two genera is not a question of which aspect of the polyzoarium is 
 cell-bearing, but of the arrangement of these cells on the branches. 
 
 It is, however, to Polypora, as pointed out by Dr. Waagen, as well as to Phyllopora, 
 that Protoretepora is most nearly allied. Here the arrangement of the cells on the 
 interstices is identical, the only question being as to which aspect of the polyzoarium is 
 celluliferous. In Protoretepora it is undoubtedly the inner. I quite agree with Dr. 
 Waagen as to the close affinity of Polypora and Protoretepora ; but before they can be 
 united it must be shown that in the type species on which McCoy established the former, 
 the polyzoarium is celluliferous on the inner face, and in consequence therefore infundi- 
 buliform. Until this is demonstrated Protoretepora can be satisfactorily made use of as 
 a genus. I cannot agree with Dr. Waagen that the question of this, or that face being 
 cell-bearing, is one of accident. He says—“ The sole difference between the two consist- 
 ing in the circumstance, that in the one the pores are said to be placed on the inner, in 
 the other on the outer side of the funnel-shaped colony. Such a position of the pores is 
 evidently only accidental, depending upon the mode in which the quite young and still 
 fan-shaped colony first became twisted ; if towards the poriferous side the pores remained 
 on the inner side, if in the reverse direction the pores remained outside.”* That “the 
 position of the pores is evidently accidental” is pure assumption, and it has yet to be 
 proved that these infundibuliform genera commenced life asa “still fan-shaped colony,’ 
 and not with a miniature infundibuliform or cup-shaped outline. I much question if the 
 mode of growth is not a regular and constant factor in the anatomical construction of 
 such genera. It certainly is constant in a large number of recent Polyzoa, examined 
 for the purpose by Mr. T. Whitelegge, of the Australian Museum, and the Writer. 
 Taking Retepora as an example of the more or less infundibuliform solitary polyzoaria, 
 we pod that the inner aspect was invariably celluliferous in both 2. monilifera, 
 Macq., the Port Phillip form, and &. jacksoniensis, Busk., inhabiting Port Jackson, 
 and the outer side of the polyzoarium never. The same is the case in such tube-like 
 species as Mucronella delicatula, Busk., and M. bisinuata, Smith, from Thursday 
 Island, and also Schizoporella australis, Hasw. The fact is again repeated in the sub- 
 dendroid species of Cellepora, and in saucer-shaped polyzoaria, like Carbasea cribiformis. 
 
 One very essential character ascribed by De Koninck to his genus appears to have 
 been overlooked by Dr. Waagen. The former says of Protoretepora, “ toute la surface 
 interne est ornée de plusieurs lignes de petites cellules.”’ Now, whatever the celluliferous 
 aspect may have to do with generic separation, we have here a feature, which on Dr. 
 Waagen’s own showing is of importance, for, he says, speaking of Polypora, “the 
 pores restricted to the branches.’ Until, therefore, McCoy’s type species of Polypora 
 can be shown to be celluliferous on the inner aspect, and in the case of both Phyllopora 
 and Polypora on the dissepiments as well as the interstices, De Koninck’s genus can 
 retain its rank as such. 
 
 PROTORETEPORA AMPLA, Lonsdale, sp. 
 
 Fenestella ampla, Lonsdale in Darwin’s Geol. Obs. Vole. Islands, 1844, p. 163. 
 3 Lonsdale in Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 268, t. 9, ff. 3a-d. 
 Dana, Geology Wilkes’ U.S. Explor. Exped., 1849, p. 710, b 12, ff. Land Ja, 
 Pe oora ga. Etheridge fil., Trans. R. Soc. Vict., 1876, xii., p. 66, Pl., 
 Protoretepora ampla (pars), Etheridge fil., Cat. casteatian Foss., 1878, p. a : 
 Sp. Char. Polyzoarium fine or cup-shaped, with the upper portions more or 
 less crumpled. Interstices broad, flattened, and expanding previous to bifurcation ; 
 
 dissepiments short, sometimes celluliferous. Jenestrules oval, and rather long, the 
 
 
 
 
 
 
 
 * Pal. Indica (Salt Range Foss.), 1885, Ser. xiii., No. 1, fase. 5, p. 775. 
 
222 
 
 margins sometimes irregular, or wavy from the projection of the lateral rows of cell- 
 mouths. Cellules round, exsert, in from three to ten oblique rows, separated by slightly 
 impressed lines or grooves. Outer surface of polyzoarium granular-striate. 
 
 Obs. Inaformer Paper * it was shown that my Colleague had collected three well- 
 
 marked forms of retiform Polyzoa from the Carboniferous rocks of Northern Queensland. 
 One of these was a large crumpled form, to which the name Protoretepora Koninckit 
 was given; the second was stated to be allied to P. ampla, but smaller in habit ; whilst the 
 third was ee fossula, Lonsd. At the same time the great difficulty aiendiae the 
 satisfactory determination and separation of these species was pointed out. 
 
 Since the remarks referred to were written, I have found, in the National 
 Collection,+ Strzelecki’s types of P. ampla, Fenestella fossula, and F. internata, described 
 by Lonsdale. A comparison of these types with the Queensland specimens has rendered 
 a revision of the names applied to the latter necessary. In the first place the coarse 
 form called P. Koninckii can only be regarded as an extreme variety of the typical 
 P. ampla. Secondly, the fossil compared to the latter is another variety, but in the 
 opposite direction to P. Koninckii, being of a finer and smaller habit ; whilst, in the last 
 place, the fossil called Fenestella fossula, I believe to be that species. 
 
 The leading features of Protoretepora ampla, therefore, are the coarseness of its 
 mesh, and the want of clear demarcation between the dissepiments and interstices. The 
 former varies in its greatest extent towards the var. Koninckii, and in the least degree 
 towards the other condition, which will be immediateiy described as the var. Woodsit. 
 
 Loc. and Horizon. Blackfellows’ Diggings, near Rockhampton (The late R. 
 Daintree; Colln. British Museum); Gympie (2. ZL. Jack); Foot of Broadsound 
 Ranges, between Maxford and Apis Creek, about Lat. 22° 52’ S., and Long. 149° 34! E. 
 (J. MW. Kaufmann)— Gympie Beds. 
 
 PROTORETEPORA AMPLA, var. Woopsil, var. nov., Pl. 8, fig. 12. 
 
 Protoretepora ampla, De Koninck (non Lonsdale), Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 180, t. 8, 
 f, 5a-c. 
 sp. ind., Etheridge fil., Proc. R. Phys. Soc. Edinb. 1880, v., p. 278. 
 
 Obs. As before stated, this name is applied to that form believed to be a small 
 variety of P. ampla, and typified by Prof. De Koninck’s figure, which is certainly not 
 that of the species proper. The entire habit of the polyzoarium is on a smaller scale 
 than that of Lonsdale’s type specimen, but the details of structure are otherwise 
 identical. 
 
 Loe. and Horizon. Coral Creek, below Sonoma Road-crossing, Bowen River 
 (R. L. Jack) —Middle or Marine Series of the Bowen River Coal Field. 
 
 La) 
 
 PROTORETEPORA AMPLA, var. Kontnoxut, Etheridge fil. 
 Protoretepora Koninckit, Etheridge fil., Proc. R. Phys. Soc. Edinb. 1880, v., p. 277. 
 
 Obs. The polyzoarium is infundibuliform, curled, and much crumpled, and of 
 large extent. The fenestrules are small, round, separated by wide interspaces 
 (interstitial), and arranged in quincunx. Interstitial surface occupied by from five to 
 ten rows of cell-apertures between contiguous fenestrules. Cells with hexagonal or 
 polygonal bases. Basal plate thin and striated. 
 
 The fenestrules are smaller than in typical specimens of P. ampla, Lonsdale, 
 but the increased interstitial surface separating the circular fenestrules gives to P. ampla, 
 
 
 
 * Proc. R. Phys. Soc. Edinb., 1880, v., p. 274. 
 + In the Geological Department, British Museum (Natural History), London. 
 
223 
 var. Koninckit, a very marked appearance, which is still further increased by the large 
 extent of the curled and crumpled infundibuliform frond, with its numerous ramifications, 
 displayed to great advantage in the nodular matrix in which it is entombed. 
 Loc. and Horizon. Coral Creek, below Sonoma Road-crossing, Bowen River, in a 
 decomposed nodular ironstone, associated with Stenopora, and numerous other fossils 
 
 (R. L. Jack)—Middle or Marine Series of the Bowen River Coal Field. 
 
 Family—THAMNISCID 2. 
 Genus—GLAUCONOME (Miinster), Lonsdale, 1839.* 
 
 (Miinster in Goldfuss. Petrefacta Germanie, 1826, i., p. 217; restricted, Lonsdale, Murchison’s Silurian 
 Syst., 18389, p. 677.) 
 
 Obs. In “ Notes on Carboniferous Polyzoa,’+ I have fully discussed the value 
 of the generic name Glawconome and re-defined it. Since my remarks were made, Mr. 
 G. R. Vine has proposed a new genus { to take the place of the present one, but it seems 
 to me on very insufficient grounds. After a careful perusal of his remarks, I am quite 
 unable, with the present means at my disposal, to comprehend his very disjointed and 
 indefinite Memoir. 
 
 GLAUCONOME, sp. ind., Pl. 44, fig. 11. 
 
 Obs. But a single specimen of this genus has come under my notice amongst 
 the Queensland fossils, and that is only a fragment. It consists of a main stem, with 
 two primary branches, which are pinnate, with supplementary branchlets between them ; 
 but as only the reverse, or non-celluliferous face is presented to view, the species 
 cannot be determined. 
 
 Loc. and Horizon. Rockhampton District § (OC. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 Family—PETALOPORID&. || 
 
 Obs.. Mr. E. O. Ulrich ¥ has included the genus Rhombopora, Meek, in the 
 Rhabdomesontide, with the peculiar genus Rhabdomeson, Young and Young, and it 
 seems to me very improperly so. Rhabdomeson is one of the few Polyzoa possessing a 
 solid axis. This is also known to exist in the living Rhabdopleura, Allman, and, accord- 
 ing to Ulrich, is again met with in two other Paleozoic genera, Celoclema, Ulrich, and 
 Cheilotrypa, Ulrich. 
 
 The presence otf a cylindrical chitinous rod in Rhabdoplewra has been thought of 
 sufficient importance, together with other characters, to warrant the erection not only of 
 a separate family, but even of a distinct class for its reception. The remarks of Dr. 
 
 
 
 
 
 
 
 * Non Glauconome, Gray, 1828, a genus of Pelecypoda. 
 + Ann. and Mag. Nat. Hist., 1877, xx., p. 30. 
 { Brit. Assoc. Report for 1883 [1884], p. 191. Whilst referring to this ‘‘ Report,” I wish to correct 
 two very unnecessary errors into which Mr. Vine has fallen with regard to species of mine. Under 
 
 Thamniscus (p. 195), is mentioned 7, Rankinei, Young and Young. Had Mr. Vine paid the slightest 
 attention to my paper quoted above, and which he mentions in his bibliography, he would have found this 
 to be a synonym of my Zhamniscus pustulata, at one time described by me as Polypora. I there entered 
 fully into this subject, showing how the Messrs. Young, of Glasgow, had fallen into the same mistake. The 
 next point is that a remarkably good species of Fenestella, described by me as F’, scotica, is relegated, solely 
 on Mr, Vine’s authority, to another of my species, /, tuberculocarinata, as a synonym, Itis almost needless 
 to remark that they are distinct. 
 
 § See note, p. 199. 
 
 || Petaloporide, Waagen. 
 
 { Journ, Cincinnati Soc, Nat. Hist., 1884, vii., p. 24. 
 
224 
 
 . 
 
 Hincks,* in his description of Rhabdopleura, bear very pertinently on this point. He 
 says—‘ The relation of the polypide to its dwelling in Rhabdopleura is totally unlike 
 that to which we are accustomed in the ordinary polyzoon. . . . . The polypide is 
 therefore wholly unconnected with its cell. . . . Its only connection is with a 
 cylindrical chitinous rod, enclosing a soft cellular core, and traversing the whole of the 
 adherent portion of the zoarium.” 
 
 This anomalous structure is not present in Rhombopora, and I must confess to 
 being quite at fault in attempting to account for Mr. Ulrich’s reason for placing such 
 widely different genera in the same family. Under these circumstances the above 
 family is adopted after Waagen. 
 
 By Zittel+ this genus has been placed in the Cerioporide, but this is equally 
 inadmissible. I have already called attention {to the probability that the British 
 Carboniferous Polyzoon named Ceriopora interporosa, Phill., and C. sémilis, Phill., were 
 referable to Rhombopora, and I am glad to find that Mr. Ulrich confirms my opinion as 
 regards the former after an examination of its microscopic structure. 
 
 Genus—RHOMBOPORA, Meek, 1872. 
 (Hayden’s Report E. Nebraska, p. 141). 
 
 Ruompopora taxa, Etheridge, sp., Pl. 9, figs. 8 and 9. 
 
 Ceriopora ? laxa, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 332, t. 25, f. 2 and 2a, 
 Rhombopora ? laxa, Etheridge fil., Cat. Australian Foss., 1878, p. 46. 
 
 Sp. Char. Polyzoarium loosely dendroid ; branches sub-cylindrical or compressed, 
 bifurcating twice or thrice; cell-apertures small, equal, apparently round, and opening 
 obliquely upwards and outwards, arranged in quincunx. Spiniform tubuli not observed. 
 
 Obs. Mr. R. Etheridge, F.R.S., who described this species, states that it 
 possessed affinity with Rhombopora serialis, Portlock,§ from the Carboniferous rocks of 
 Hook Point, Wexford, although the cell-apertures are neither so densely nor so regularly 
 arranged as in that species. My Colleague has obtained what may be considered a large 
 variety of this species, differing, however, in no other particular than that of size from 
 the original specimens. . lara has hitherto been met with only as natural sections, 
 and the surface characters are in consequence unknown. 
 
 Loc.and Horizon. Gympie (Lhe late R. Daintree and R. L. Jack) ; Rhynchonella 
 Creek, Stanwell, near Rockhampton (Lhe late James Smith)—Gympie Beds. 
 
 The Polyzoa in the green chloritic rock of Gympie are seldom recognisable, but 
 are usually preserved merely as black or very dark, apparently carbonaceous, stains, and 
 are therefore more than ordinarily difficult to determine. In addition to Protoretepora 
 ampla, there is a form with a strong resemblance to Retepora ? laxa, De Koninck,|| in its 
 irregularity of growth, but it may perhaps be only a Protoretepora rendered rough and 
 irregular by the hackly fracture of the stone. A third form, either Fenestelia or 
 Polypora, of a. stiff and rigid appearance, possessing very large, square, oblong fenestrules, 
 appears to be a characteristic species. The interstices are straight and regular, and the 
 dissepiments at right angles (Pl. 8, fig. 9). 
 
 
 
 * Hist. Brit. Marine Polyzoa, 1880, p. 577. 
 
 + Handb. Pal. Bd., i., p. 609. 
 
 + Ann. and Mag. Nat. Hist., 1887, xx., p. 30. 
 
 § Report Geol. Londonderry, Tyrone, &c., 1848, p. 327, t. 22a, f. 6. 
 
 || Foss. Pal, Nouy.-Galles du Sud, 1877, Pt. 3, t. 8, f.6 (See Pl. 8, figs. 10 and 11.) 
 
225 
 
 Genus—MYRIOLITHES, Eichwald, 1860. 
 (Lethzea Rossica, 1860, i., p. 450.) 
 
 MYRIOLITHES P QUEENSLANDENSIS, sp. nov. 
 
 Sp. Char. Polyzoarium small, with the branches oval, or more or less flattened. 
 Cells very small, round, arranged in vertical series, alternate or sub-alternate, their 
 margins rim-like or a little exsert, and somewhat more than their own diameter apart ; 
 intercellular surface vermicular striate, the strie anastomosing above and below each cell- 
 aperture, or they are at times sub-parallel to one another. 
 
 Obs. This little fossil, which occurs in fragments on the surface of weathered 
 limestone, has given me much trouble, but accords better with Eichwald’s description of 
 Myriolithes than with any other similar genus with which I am acquainted. I have, 
 however, failed to detect any intermediate capillary tubes. It is allied to WZ. monticola, 
 Eichwald, from Carboniferous Limestone of the Oural, but differs in its method of 
 branching, and in the form and arrangement of the cells. I have not yet examined 
 sufficient material to warrant my assigning it to any particular family. 
 
 Loc. and Horizon. Blenavon, Lilymere, near Rockhampton (The late James 
 Smith); Lilymere Marble—Gympie Beds.* 
 
 Section—MOLLUSCA VERA. 
 Class—BRACHIOPODA. 
 
 Order—TRETENTERATA, 
 Family—TEREBRATULID 2. 
 
 Genus—DIELASMA, King, 1850. 
 (Mon, Perm. Foss. England, p. 146.) 
 
 DIELASMA CYMB@FoRMIS, Morris, Pl. 9, figs. 10 and 11. 
 
 Terebratula eymbeformis, Morris in Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 278, t. 17, 
 ff. 4and 5. 
 biundata, McCoy, Ann. and Mag. Nat. Hist., 1847, xx., p. 231, t. 18, f. 9. 
 sacculus, var. hastata (pars) Etheridge fil., Cat. Australian Foss., 1878, p. 61. 
 sacculus, var. cymbeformis, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 8, 
 p. 255, t. 15, f. 4 and 4a. 
 Obs. On the publication of the “‘ Catalogue of Australian Fossils,” I,in common 
 with others, believed this to be only a form of the ordinary D. sacculus, so characteristic 
 of Carboniferous rocks, but the acquisition of other specimens now leads me to a 
 contrary opinion. The shell generally is more attenuated and higher towards the 
 umbonal region of the ventral valve, much more overcurved, and the shoulders longer and 
 more pronounced. The foramen is vastly larger in comparison with the size of the 
 shell, much more truncate and horizontally placed. The dorsal valve is arched in a 
 greater degree, becoming in some examples sub-angular towards the umbo. Lastly, the 
 lateral margins of the united valves are always more sinuated. For the reason now 
 stated, I believe D. hastata, Sby., and D. cymbeformis should be retained as separate 
 species. With the exception of the unusually large specimen of D. hastata figured by 
 
 * Also reported by Mr. Smith, from the Limestones at Dalma (Rockhampton District) and Raglan 
 (Port Curtis District), but I much question its occurrence at the latter locality. (R, #. Junr.) 
 
 ay 
 
226 
 
 the late Dr. T. Davidson,* this shell is probably one of the largest of the Upper 
 Paleozoic Terebratule known. The British specimen measures two and three-quarter 
 inches in length, two inches in breadth, and one and a-half in depth. The present shell, 
 on the contrary, is two and a-half inches long, and two inches in breadth, but the depth 
 is reduced to a quarter of an inch. In the high shoulders of the ventral valve, and size 
 and position of the foramen, there is a strong resemblance to D. elongata, Dana.t 
 But the lateral margins in this species are much curved concavely, not sigmoidally, and 
 the front margin was probably entire. The curvature of the shell in the present species 
 is well displayed both in Morris’s and De Koninck’s figures, whilst in the former are also 
 shown the impressions of the strong dental plates, equally well seen in our specimen. 
 The form of the foramen is likewise well preserved, even to the entire margin. 
 
 Loe. and Horizon. Mouth of Coral Creek, Bowen River Coal Field (HZ. Edelfelt) 
 —Middle or Marine Series of the Bowen River Coal Field. 
 
 DrenasMa saccuuus, Jlartin, var. 
 
 Conch. (Anomites) sacculus, Martin, Pet. Derb., 1809, p. 14, t. 46, f. 1 and 2. 
 
 Terebratula sacculus, Davidson, Mon. Brit. Carb. Brach., 1857, Pt. 1, p. 14, t. 1, f. 23, 24, 27, 29, 30. 
 
 Dielasma sacculus, De Koninck, Faune Cale. Carb. Belgique, 1887, Pt. 6, p. 27, t. 6, ff. 14-17, 19-26, 35-45, 
 t. 7, £. 60-77. 
 
 Sp. Char. Shell obovate, depressed, concavo-convex, especially towards the 
 front, which is not sinuated. Ventral valve depressed, convex, becoming flat and 
 narrowed towards the front. Dorsal valve convex immediately below the umbone, 
 becomes flattened, and then concave as the front is approached. Length, two inches and 
 three-quarters ; breadth, one inch and three-quarters. 
 
 Obs. The depressed boat-shaped outline, and its extreme shallowness as compared 
 with its length and breadth, are very marked features in this shell. The surface of the 
 ventral valve carries a few indistinct concentric furrows. The lateral marginal curve of 
 the valves is very slight. In outline we here have a distinct resemblance to the little 
 variety termed by Davidson gillengensis,t but the great difference in size will at once 
 distinguish our shell. , 
 
 Loc. and Horizon. Banana Creek, near Banana, Dawson River (H. Mackay ; 
 Colln. De Vis)—Middle or Marine Series of the Bowen River Coal Field. 
 
 DIELASMA SACCULUS, var. HASTATA, J. de C. Sowerby. 
 
 Terebratula hastata, J. de C. Sby., Min. Con., 1824, v., p. 66, t. 446. 
 Aa a5 Davidson, Mon. Brit. Carb. Brach., 1857, Pt. 1, p. 11, t. 1, ff. 1-12. 
 sacculus, var, hastata, De Koninck, Rech. Foss. Pal. Nouv.-Galles du Sud, 1877, Pt 3, p. 257, 
 t. 15, ff. 3 a-f. 
 Dielasma hastatum, De Koninck, Faune Cale. Carb. Belgique, 1887, Pt. 6, p. 9, t. 3, ff. 1-26, etc. 
 
 Obs. A single small and worn, but almost complete example of this variety of 
 the above protean species has been met with. There seems to be little or no sinuosity 
 in the front margin, the ventral valve is very much flattened, and the dorsal valve more 
 arched. Beyond the general outline there are no characters which can be seized upon 
 for description. 
 
 Loe. and Horizon. Rockhampton District § (C. W.De Vis; Colln. De Vis)— 
 
 Gympie Beds. 
 
 2? 
 
 * Mon. Brit. Carb. Brach., 1880, iv., Pt. 3@%. 30, f. 17a and b. 
 
 + Geology Wilkes’ U. S. Explor. Exped., 1849, x., Atlas, t. 1, f. 3a, 
 £ Davidson, loc. cit., p. 17, t. 1, figs. 18-20, 
 
 § See note, p. 199, 
 
227 
 
 DrietasMa, ? sp. ind., Pl. 40, figs. 1 and 2. 
 
 Obs. This very remarkable form resembles an unnamed shell figured by Dana * 
 in the general form and proportion of its valves. Theshell is long-oval, with much 
 compressed valves, the ventral very slightly convex, the dorsal nearly flat immediately 
 below the umbone, becoming more or less concave towards the front; the valve margins 
 are not in any way sinuous, but simply gradually curved. 
 
 It certainly cannot be referred to D. cymbeformis, but corresponds, so far as mere 
 outline is concerned, with D. gillengensis, Davidson,t but the difference in size is remark- 
 able, and the valves of the present Brachiopod are narrower forwards. Another of 
 Dana’s species, D. amygdala,t although again smaller in size, has a very depressed 
 dorsal valve, and is to some extent like it. 
 
 It is even questionable whether it be correctly referred to Dielasma, as the 
 surface of the ventral valve shows signs of a long septum. It is a very puzzling form, 
 and would appear to resemble some of the Devonian Terebratulide rather than those of 
 higher Paleozoic rocks. 
 
 Loe. and Horizon. Rockhampton District § (0. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 Family—SPIRIFERID@. 
 
 Genus—SPIRIFERA, J. Sowerby, 1816. 
 (Min. Con., ii., p. 41.) 
 
 Obs. No more difficult group exists in the Australian Permo-Carboniferous 
 Series than the Spirifers. So many species have been made on fragments, and the 
 presence of European species so frequently determined on indifferent specimens, that it 
 has become almost impossible to establish with certainty what species do exist. I hope, 
 however, to unravel this confusion when the study of the large series of New South 
 Wales specimens is undertaken. In the meantime the following determinations must 
 be accepted as a temporary solution of the Queensland species, although I am anything 
 but satisfied with it. 
 
 SpPrrIFERA sTRIATA, Martin, sp., ? Pl. 9, fig. 16. 
 Spirifera striata (Martin), Davidson, Mon. Brit. Carb, Brach., 1857, Pt. 1, pp. 19 and 246, t. 2, ff. 12-21. 
 He » Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 334, t..17, f. 5. 
 
 Obs. The mesial fold is not so well defined as in the typical S. striata, and some 
 transverse forms of S. bisulcata assume this shape. We may, however, confidently refer 
 it to the above shell, or one of its many varieties. 
 
 This most variable and widely distributed species of the genus Spirifera appears 
 to be not uncommon, as I have been given to understand that individuals of the species 
 are abundant in the Bowen River Series. (Htheridge.) 
 
 Without for a moment venturing to deny that this may be Spirifera striata, it 
 at the same time appears exceedingly doubtful. The ribs are much too few in 
 number, do not possess the angular sharp outline of S. striata, and the sulcus seems 
 to be quite plain. The specimen was evidently a very imperfect one, and the cardinal 
 angles may have been either acute or rounded. It is, in fact, impossible to say what 
 
 * Geology Wilkes’ U. S. Explor. Exped., Atlas, t. 1, f. 4d. 
 + Mon. Brit. Carb. Brach., 1857, Pt. 1, t. 1, f. 18-20, 
 
 + Dana, loc. cit., t. 1, f. 2d, 
 
 § See note, p. 199 
 
228 
 
 the species was. For my own part, I cannot say that a Spirifera which could be 
 definitely referred to the present species has ever come under my notice from Queens- 
 land rocks. 
 
 Loc. and Horizon. “ Bowen River, Peak Downs” * (The late R. Daintree)— 
 Middle or Marine Series of the Bowen River Coal Field. 
 
 SPIRIFERA, sp. ind. (a.), Pl. 9, fig. 12. 
 
 Spirifera, allied to S. striata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 336, t. 18, f. 8. 
 (Compare Spirifera ywennamensis, De Koninck in Dumont D’Urville, Voy. au. Pole Sud, Géologie, 
 Atlas, 1846, t. 9, f. 19-21.) 
 
 Sp. Char. Cardinal margin of dorsal valve long and straight; area moderately 
 large; alar angles rounded; fold wide and prominent, but not angular, rounded and 
 plain, expanding rapidly towards the front, bounded on each side by a marked depres- 
 sion or groove. From twelve to fifteen simple, flattened, curved ribs ornament the 
 lateral portions of the valve, and are crossed by lamin of growth, which are also con- 
 spicuous on the fold. 
 
 Obs. This shellis only known to me in the céndition of decorticated casts of 
 the dorsal valve, averaging in size from one to one and a-quarter inches long. The 
 chief points of interest are the plain fold, and the simple, flattened riblets. It is a very 
 interesting species, which I have, so far, been unable to determine, but the general 
 appearance of the specimens is well conveyed by the figure given by Mr. Etheridge, as 
 above quoted. TI have described the fold as plain, but on two of the specimens before 
 me there is a faint division perceptible, in others its surface is quite unbroken; no 
 great amount of convexity could have existed in this valve. The published figure does 
 not convey to me the idea of Spirifera striata at all, nor do I think it can be so 
 referred, the riblets being much too wide for the size of the valve. 
 
 The figure of De Koninck’s 8. yuennamensis, published by D’Orbigny, closely 
 resembles the specimens from Rockhampton, only the former is much larger, and the 
 ribs are less in number, only nine on each side; the comparison is, however, worth 
 entertaining. The sulcus on each side the fold is a marked feature, and should assist 
 in identification. 
 
 Loc. and Horizon. Don River (Lhe late R. Daintree)—Gympie Beds ; Rock- 
 hampton District + (0. W. De Vis; Colln. De Vis)—Gympie Beds. 
 
 SPIRIFERA VESPERTILIO, G. B. Sowerby, Pl. 10, fig. 8. 
 Spirifera vespertilio, G. B. Sowerby in Darwin’s Geol. Obs. Vole. Islands, 1844, p. 160. 
 
 in af Morris in Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 282, t. 17, f. 1 and 2 
 (? excl. f. 3.) 
 *3 55 Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 329, t. 16, f. 2. 
 
 Obs. Ill-preserved Spirifere, probably referable to this species, have been met 
 with at two localities. Respecting the specimen figured by Mr. Etheridge, he says— 
 “Tt has not the number of ribs described by Sowerby; but their angular, imbricated, 
 or fimbriated condition, the width of the mesial fold or ridge, and the pointed beak, with 
 the transversely fusiform shape of the one valve, are sufficient to warrant my retaining 
 this name for the specimen from Gympie.” He adds— Five or six rows of .acutely 
 angular imbrications are distinguishable upon the mesial fold, and traceable along the 
 attenuated lateral wings of the cardinal angles.” 
 
 
 
 * Probably ‘“‘Bowen River” is correct, The Bowen River is not included in the Peak Downs 
 District. (R.Z.J.) 
 + See note, p. 199, 
 
229 
 
 In addition to the above, the late Mr. James Smith has obtained, at Stanwell, a 
 small Spirifera, possessing a lengthened hinge-line, flattened wings, an angular dorsal 
 fold, and sharp ribs visible near the front margin. Such characters would indicate 
 it to be a young form of S. vespertilio. 
 
 Loe. and Horizon. Gympie (The late R. Daintree); Stony Creek, Stanwell, near 
 Rockhampton (The late James Smith)—Gympie Beds. 
 
 SPIRIFERA convoLuTa, Phillips, Pl. 10, figs. 10 and 11. 
 
 Spirifera convoluta, Phill., Ill. Geol. York, 1836, ii., p. 217, t. 9, f. 7. 
 ” Py Davidson, Mon. Brit. Carb. Brach., 1857, Pt. 1, p. 35, t. 5, f. 2-15 (for general synonymy). 
 a i ? Etheridge, Quart. Journ. Geol. Soc., 1872, xxvili., p. 335, t. 17, £. 3. . 
 9 Ay Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 280, t. 7, f. 6. 
 
 Obs. The most satisfactory example of this species yet obtained in Queensland 
 has been figured by Mr. R. Etheridge, F.R.S., who remarked on it—‘‘ We may refer 
 this fragment to Sp. convoluta, its extreme width and straight hinge-line essentially ally 
 it to this shell; the acute angles at the extremities are lost, still many of our Yorkshire 
 shells strongly resemble this species; the ribs on the mesial fold are also less defined 
 than on most typical forms.” 
 
 Loc. and Horizon. Bowen River (The late R. Daintree) ; Parrot Creek, four and 
 a quarter miles up Bowen River (2. L. Jack)—Middle or Marine Series of the Bowen 
 River Coal Field. ; 
 
 SPLRIFERA LATA, McCoy. 
 Spirifera lata, McCoy, Ann, and Mag. Nat. Hist., 1847, xx., p. 233, t. 13, f. 7. 
 Spirifer latus, De Koninck, Foss, Pal. Nouy.-Galles du Sud, 1877, Pt. 3, p. 244. 
 
 Obs. It is with considerable hesitation that I introduce this as a Queensland 
 species. I have not yet seen a specimen either from this Colony or from New South 
 Wales possessing smooth alar expansions in connection with as large a number of ribs 
 as described by McCoy. On the other hand, here are several in which the wings are 
 certainly devoid of coste, and the bodies of the shells bearing nine instead of from 
 sixteen to eighteen. The cardinal margin is long with acute angles, and the lateral 
 portions of the valves spreading and wing-like. The fold is very prominent, high 
 towards the front, and appears to have been divided by a narrow groove. The sinus 
 furrows the ventral umbone quite from its apex, gradually spreading out towards the 
 front, where it is wide and moderately deep. Particularly well-marked growth-lamine 
 crossed the valves longitudinally. . 
 
 The wings are not devoid of ribs to the same extent as McCoy’s representation of 
 S. lata, but still sufficiently so to become a point of importance in the determination of 
 the species. The plain fold and sinus at once separate these shells from Spirifera 
 vespertilio, whilst the simple cost are equally important in distinguishing them from 
 S. convoluta. 
 
 Loc. and Horizon. Yatton Gold Field (R. L. Jack)—Gympie Beds; Banana 
 Creek, near Banana (D. Mackay; Colln. De Vis)—Middle or Marine Series of the 
 Bowen River Coal Field. 
 
 Sprrirera CrarKet, De Koninck, Pl. 10, fig. 16.? 
 Spirifer Clarkei, De Koninck, Foss, Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 236, t. 13, ff, 2, 2a. 
 
 Obs. Our knowledge of this good species, as a Queensland shell, depends upon 
 a decorticated specimen which I cannot otherwise refer. The sinus of the ventral valve 
 is quite devoid of ribs, but possesses from twelve to thirteen simple ones on each 
 
230 
 
 flank ; the umbo is prominent and sharp. The fold of the dorsal valve is proportionately 
 narrower than in De Koninck’s illustration, and there are faint indications of slight 
 ribs, but these are the only points in which our specimen differs from 8. Clarkei. Both 
 valves bear traces of strong concentric lamine. 
 
 Loc. and Horizon. Stonehumpy Creek, Bowen River (Z. Edelfelt)—Middle 
 or Marine Series of the Bowen River Coal Field. 
 
 SPIRIFERA TRIGONALIS, Martin, sp. 
 
 SPIRIFERA TRIGONALIS, var. BISULCATA, J. de C. Sowerby, Pl. 9, fig. 15. 
 Spirifera bisulcata, J. de C. Sby., Min. Con., 1825, v., p. 152, t. 494, ff. 1, 2. 
 trigonalis, var. bisulcata, Davidson, Mon. Brit. Carb. Brach., 1857, Pt. 1, p. 31, t. 5, f. 1,"t. 6, 
 
 f, 1-19, t. 7, f. 4; Ibid., 1862, Pt. 5, p. 222. 
 
 ‘3 allied to S. bisulcata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 335, t. 17, f. 4. 
 Spirifer bisulcatus, De Koninck, Foss. Pal. Nouy.-Galles du Sud, 1877, Pt. 3, p. 246, t. 14, f. 5. 
 
 Obs. Both in the Permo-Carboniferous rocks of New South Wales and Queens- 
 land, a Spirifera occurs, sometimes acquiring considerable dimensions, and possessing 
 many of the characters of the common SN. bisuleata. The coste in this species are very 
 characteristic, and are either flat or flatly rounded, close to one another, and frequently 
 bisuleate. Both the fold and sinus are similarly occupied. The coste and intercostal 
 Spaces are minutely and longitudinally striate, and, when in a good state of preservation, 
 very minute and very wavy. Similar lines can be detected accompanying the lines of 
 growth in a transverse direction. This is a marked feature in S. disulcata, and equally 
 so in the Queensland shells. The latter appear to me to be less convex and gibbous 
 than the present variety of Martin’s shell, and in some points almost to agree better 
 with the var. crassa, De Koninck. Although the tendency of the ribs to arrange them- 
 selves in three groups on the fold is not to any great extent marked, it is still apparent. 
 In two of our specimens the long reniform vascular impressions are well displayed, and 
 as I do not remember to have seen an illustration of this anatomical point in S. biswlcata, 
 a figure of it is given. 
 
 Loc. and Horizon. Bowen River (Lhe late R. Daintree)—Middle or Marine 
 Series of the Bowen River Coal Field ; Rockhampton District * (C. W. De Vis; Colln. 
 De Vis)—Gympie Beds. 
 
 29 
 
 SPIRIFERA TRIGONALIS, ? var, AcUTA, Htheridge, Pl. 10, fig. 12. 
 Spirifera bisulcata, var. acuta, Ktheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 329, t. 16, f. 1. 
 
 Obs. The varietal name acuta was applied by Mr. R. Etheridge, F.R.S., toa 
 shell which appears to differ from ordinary forms of S. ¢rigonalis and its varieties, in 
 its much fewer and simpler ribs, and grooved fold. I am not prepared to offer any 
 suggestion as to its identity other than the above. 
 
 Loc. and Horizon. Gympie (The late Rk. Daintree)—Gympie Beds. 
 
 SPIRIFERA TRIGONALIS, var. CRASSA, De Koninck, Pl. 11, fig. 5. 
 
 Spirifer crassus, De Koninck, Rech. Anim. Foss. Terr. Carb. Belgique, 1848, p. 262, t. 15 bis, f. 5. 
 Spirifera crassa, Davidson, Mon. Brit. Carb., Brach., 1857, Pt. 1, p. 25, t. 6, f. 20-22, t. 7, f. 1-3. 
 
 trigonalis, var. crassa, Davidson, loc. cit., 1862, Pt. 5, p. 222. 
 
 Obs. We have before us (Pl. 11, fig. 5) a portion of a large decorticated 
 Spirifera, resembling in general outline and appearance Martiniopsis subradiata, Morris, 
 but with the exterior bearing the almost flattened ‘‘ rounded, unequal, bifurcated, or 
 
 * See note, p. 199. 
 
231 
 
 intercalated ribs ’’ both on the fold and sinus of De Koninck’s shell, as described by 
 Davidson; and not “ with a few undefined, and numerous faintly elevated ridges more 
 visible in the cast,’ as seen in the former and Australian species. IL subradiata at 
 times assumes very large proportions and possesses, on the cast, many indistinct, simple, 
 radiating ridges, and notwithstanding the unequal bifurcating nature of those on 8. 
 crassa, it is, of course, just possible that we may be dealing only with an extreme 
 variety of our common form, although I am much more inclined to take the other view. 
 Neither do I believe that it is in any way related to the shell figured by Professor De 
 Koninck as Spirifera pinguis, var. rotundata,* in which the ribbing is broad, more or 
 less equal, with but little interpolation, whilst the fold and sinus are comparatively 
 devoid of ribs. 
 
 Loe. and Horizon. Stony Creek, Stanwell, near Rockhampton (Lhe late James 
 Smith)—Gympie Beds. 
 
 SPIRIFERA DUBIA, Etheridge, Pl. 10, fig. 14. 
 Spirifera dubia, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 330, t. 16, f. 6. 
 
 Sp. Char. Shell transversely semi-circular; hinge-line nearly as long as the 
 width of the shell; cardinal angles gently rounded; mesial fold having many small ribs, 
 and wide at ventral border of shell; eight or nine ribs occur on each side of the mesial 
 fold upon the cardinal angle or lateral portion of the shell, and some of the ribs upon the 
 lateral areas bifurcated as they approached the ventral margin. (theridge.) 
 
 Obs. This shell resembles some forms of Spirifera undulata, but the ribs are 
 finer than in normal forms of that species; the ribbed mesial fold and bifurcating 
 lateral ribs are essential points of difference. Not having any outer shell, we have no 
 means of determining any markings upon the valves ; but it differs from known species 
 of Spirifera. I know of no species, either Devonian or Carboniferous, to which the 
 above shell can be referred, the rounded cardinal angles and almost semi-circular dorsal 
 valve distinguishing it from every known form. (Ltheridge.) 
 
 Loc. and Horizon. Gympie (Lhe late R. Daintree)—Gympie Beds. 
 
 SPIRIFERA, sp. ind. (b.), Pl. 88, figs. 4-6. 
 
 Spirifer vespertilio, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, t. 13, f. 40 and c (excl. f. 4a 
 and b); t. 14, f. 3?--(non G. B. Sowerby). 
 
 Sp Char. Shell oblong-triangular ; valves unequally convex ; cardinal margin 
 _ almost as long as the valves, but the alar angles rounded; front margin laterally in one 
 plane, much sinuated in the middle line. Ventral valve convex, with a well-defined deep 
 sinus extending some distance forward; shoulders high; umbo elevated and probably 
 a good deal incurved ; area wide and barely as long as the cardinal margin; fissure 
 large and triangular; cardinal muscular impressions broadly lingual; adductor scars 
 very narrow; shelly plates large and thick. Dorsal valve with the flanks only slightly 
 convex ; fold prominent, high, and wall-sided, umbo depressed. Ventral valve bears six 
 prominent, simple, straight, and somewhat unequal ribs, with a few indistinct and 
 flattened ribs in the sinus ; fold plain, the flanks of the dorsal valve bearing the same 
 number of cost ; interspaces plain and wider than the latter. 
 
 : Obs. The above characters are taken from well-preserved casts. They agree most 
 satisfactorily, and are probably identical with the short smaller form figured by De 
 Koninck as Spirifera vespertilio (loc. cit., t. 13, £.4b6 andc). Itis, however, doubtful if 
 these are G. B. Sowerby’s species of that name as figured by Morris. In the former’s 
 
 * Foss, Pal, Nouv.-Galles du Sud, 1877, Pt. 3, t. 14, t 2. 
 
232 
 
 original description it is said, “ breadth more than double its length.” Morris describes 
 S. vespertilio as “transversely fusiform” ; but, in his illustrations, Morris himself has, I 
 believe, figured two distinct species under Sowerby’s name. His figures 1 and 2 (Pl. 
 17),* are S. vespertilio, whilst fig. 3 of the same plate is another form, much shorter, 
 less triangular, and much too high a shell. Professor De Koninck, wholly ignoring 
 Morris’s description, adopts the extraordinary method of applying the name to the 
 aberrant fig. 3. His S. vespertilio is, therefore, to some extent not the species intended 
 by the earlier writers named, but is distinct, and agrees with the casts above described 
 from Queensland. If the latter, and the figures cited in De Koninck’s work are in want 
 of a name, I would propose to call them Spirifera Stutchburit, after the late Mr. 
 Samuel Stutchbury, the first Government Geologist of New South Wales, and at a 
 time when that Colony and Queensland formed one territory. The true 8S. vespertilio 
 is a long-winged, very alate shell, and quite distinct from the short triangular deltoid 
 forms now under consideration. 
 
 Loc. and Horizon. Richards’ Homestead, three miles south-west of Mount 
 Britton Township, Lat. 8. 21° 20’, Long. E. 148° 30' (4. LZ. Morisset)—Middle or Marine 
 Series of the Bowen River Coal Field. 
 
 SPIRIFERA TASMANIENSIS, Morris, Pl. 10, fig. 1, and ?15. 
 
 Spirifera rotundata, G. B. Sowerby in Darwin’s Geol. Obs. Vole. Islands, 1844, p. 159 (non Phillips). 
 Spirifer Tasmaniensis, Morris in Strzelecki’s Phys. Descrip. N. 5S. Wales, &c., 1845, p. 280, t. 15, f. 3 and 4, 
 Spirifer Tasmaniensis, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 8, p. 248, t. 9, f. 7. 
 Tasmanni (sic), Von Buch, Abhandl. K. Akad. Wissen. Berlin, 1846 [1848], p. 75, f. 3a and 6. 
 
 Obs. We possess a decorticated example, which, from its shape and general 
 appearance, seems to be this species. It is from the Bowen River Series. But, like 
 De Koninck’s figure, more ribs are present than laid down in Morris’s description. 
 Probably ten, as stated by Morris, may be regarded as the lowest number, graduating 
 up to fifteen or twenty, by counting all the bifurcations. 
 
 Another specimen possessing prominent angular ribs, united into indefinite bundles 
 of three, may also be S. tasmaniensis (Pl. 10, fig. 15). It is possible that this species 
 will prove to be only a variety of the much better marked Spirifera Stokesii. Amongst 
 extra-Australian species, compare S. musebachanus, F. Roemer,t from Texas, which is 
 very closely allied, having the same shape, clustered ribs, and highly decussated 
 appearance. 
 
 Loc. and Horizon. Stonehumpy Creek, Bowen River (2. Edelfelt); Banana 
 Creek, near Banana, Dawson River (Tne late James Smith)—Middle or Marine Series 
 Bowen River Coal Field. | 
 
 39 
 
 SPIRIFERA STOKESII, Kénig, sp., Pl. 10, figs. 2-4. 
 
 Trigonotreta Stokesti, Konig, Icones Foss. Sect., 1825, p. 3, t. 6, f. 70. 
 
 Spirtfera trapezoidalis, G. B. Sowerby in Darwin’s Geol. Obs. Vole. Islands, 1844, p. 159. 
 
 Spirifer Stokesti, Morris in Strzelecki’s Phys. Descrip. N. 8. Wales, 1845, p. 283, t. 15, ff. 1, la. 
 
 Stockesi (sic), Von. Buch, Abhand]l. K- Akad, Wissen, Berlin, 1846 [1848], p, 76. 
 
 Stokesti, D’Orbigny in Dumont D’Urville’s Voy. au Péle Sud, Géologie, Atlas, 1846, t. 9, ff. 12-14. 
 
 Sp. Char. Shell subtetragonal to trapezoidal, or deltoid, rough-looking, globose, 
 at times sub-alate, but the valves unequally convex, and the front deeply sinuate. 
 Ventral valve convex, more so than the dorsal, much produced in front, high in the 
 umbonal region; sinus broad and deep, extending well on to the umbo, which is 
 prominent and much incurved; area well marked, as long as the valve, wide; alar 
 angles rounded as a rule, occasionally bluntly pointed, on the inner surface of valve 
 
 ” 
 
 ” 
 
 * Strzelecki’s Phys. Descrip. N. S. Wales, 1845, &c. 
 + Kreidebild., Texas, 1852, p. 88, t. 11, f. 7a-c. 
 
233 
 
 much grooved and ridged; shelly plates large, strong, and thick; dental plates large, 
 extending outwards and downwards; adductor scars comparatively small, much 
 elongated ; cardinal impressions large, elongate, festoonly ridged. Dorsal valve 
 angularly convex, much produced along the middle line of the fold, which is sharp and 
 angular; umbo projecting above the area. Ornament of the valves very characteristic, 
 the flanks in both bearing four or five rough-looking costs, each composed of two to five 
 subsidiary ribs, the bifurcation taking place at about one-third from the umbones ; the 
 fold bears three slightly elevated cost on each side, and the sinus is similarly divided, 
 the whole being crossed by concentric distant, wavy, and strong imbricating lamelle of 
 growth. 
 
 Obs. The size, form, and coarse ornament are the chief points worthy of notice 
 in 8. Stokesii. The interspaces between the groups of coste, sometimes, although rarely, 
 carry smaller and subsidiary ribs. The wings are traversed by flattened, close ribs, 
 similar to the latter, but they do not project like those on the bodies of the valves. On 
 the ventral valve the costs appear at times to be less split up than those of the dorsal, 
 until contiguous to the front margin. Prof. Morris’s description is very characteristic 
 of the species. He says—“ A rough-looking species in consequence of the paucity and 
 size of the lateral ribs, the central one being still prominent.” 
 
 Spirifera Stokesii is probably the largest of the Australian radiate Spirifers, and 
 belongs to the same group as Spirifera duplicicosta, Phill.,* of the European Carboni- 
 ferous, and which possesses similar tripartite cost. The best figure of this species with 
 which I am acquainted is D’Orbigny’s. In this illustration there are three large divided 
 ribs on each flank, and the interspaces filled as previously described. The fold has 
 three ribs on each side. 
 
 Spirifera Keilhavii, Von Buch, has coarse angular ribs like our species, but the 
 form of the shell is quite different. 
 
 Loc. and Horizon. Gympie—Gympie Beds; Banana Creek, near Banana, Dawson 
 River—Middle or Marine Series of the Bowen River Coal Field ; Yatton Gold Field 
 (R. L. Jack)—Gympie Beds; Richards’ Homestead, three miles south-west of Mount 
 Britton Township (Messrs. A. ZL. Morisset and Rk. Hull)—Middle or Marine Series 
 of the Bowen River Coal Field. 
 
 SPIRIFERA PINGUIS, J. Sowerby. 
 
 Spirifer pinguis, J. Sowerby, Min. Con., 1820, iii., p. 125, t. 271. 
 
 Spirfera pinguis, Davidson, Mon. Brit. Carb. Brach, 1858, Pt. 2,-p. 50, t. 10, f. 1-12. 
 
 Spirifer pinguis, var. rotundatus, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 288, t. 14, 
 f, 2, 2a. 
 
 Obs. Numerous examples of a rather small species occur in the altered rocks 
 of the Rockhampton District, none actually perfect, but, as far as preserved, closely 
 resembling some of Davidson’s figures of the above species, particularly his figs. 1-3. 
 The ribs are rounded, one or two indistinct ones occupying the sinus, whilst the fold is 
 plain. Over and above this, the specimens, although imperfect, have that indescribably 
 rotund and rotundly-radiate appearance which always accompanies this species. 
 Davidson remarks on Spirifera pinguis— Very variable in shape, dimensions, relative 
 proportions, and degree of convexity,’ and the present shells may well come within this 
 category. ° 
 
 Loc. and Horizon. Rockhampton District t (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 
 
 * See Davidson’ s Mon. Brit. Carb. Brach., 1857, Pt. i, t. 4, f. 4. 
 + See note, p 199. 
 
234 
 
 SPIRIFERA BICARINATA, sp. 20v. 
 P10, figs 9 ands; Pl.11, figsol and abl ore 
 
 Sp. Char. Shell small, elongately triangular, very alate, and laterally extended. 
 Hinge-line much extended, straight, greater than the general width of shell. Wings 
 sharp, flattened, and narrowly triangular, with the alar angles pointed. Ventral valve 
 convex, inflated centrally, flattened at the sides. Sinus moderately broad and deep, 
 angular, bounded by prominent carina, without ribs. Umbo high, overhanging the hinge- 
 line. Area very fine and narrow. Fold. of the dorsal valve plain, and defined by deep 
 sulci, corresponding to the carinz of the ventral valve. Surface bears numerous, 
 regular, fine coste, usually simple and not often bifurcating, the interspaces bearing 
 very delicate microscopic striz, the whole crossed by occasional lamine of growth. 
 
 Obs. The characters of this little shell appear to be very constant, the extended 
 hinge-line, plain sulcus bounded by sharp carine, sharp alar angles, and the divided-off 
 fold in the dorsal valve, all render it a conspicuous and well-marked form. I am unable 
 to refer it to any knowi Australian species, whilst it possesses a considerable distri- 
 bution, and strongly recalls some Devonian forms.- Its nearest ally seems to be 
 Spirifera albapinensis, H. & W.,* from the Waverly Group of North America. 
 
 Loe. and Horizon. Corner Creck, Great Star River (2. L. Jack.) ; Gully between 
 two peaks on the left bank of the Keelbottom River, north of Old Plum-tree Inn 
 (R. LD. Jack)—Star Beds; Hawkins’ Gully, Kariboe Creek, Kroombit Diggings, Port 
 Curtis (W. H. Rands); and ? Stony Creek, Stanwell, near Rockhampton (The late 
 James Smith)—Gympie Beds. 
 
 SPIRIFERA STRZELECKII, De Koninck, Pl. 10, figs. 5-7. 
 
 Spirifera undifera, var. undulata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., pp. 330 and 331, t. 15, 
 ie Bare alr BE sy 
 Spirifer Strzeleckii, De Koninck, Foss. Pal. Nouy.-Galles du Sud, 1877, Pt. 3, p. 2385, t. 13, f. 1, t. 14, f.1. 
 
 Obs. A full description of this shell will be found in Prof. De Koninck’s Memoir, 
 but it may be incidentally mentioned in passing that his figures do not correspond in every 
 respect with those of Mr. R. Etheridge, F'.R:S., on which he established his species, but this 
 may perhaps be owing to the usually indifferent state of preservation of the Gympie 
 examples. The following observations are quoted from the original Paper:—“ The 
 Queensland specimens differ little amongst themselves, all having the well marked mesial 
 fold in the ventral valve and eight or ten ribs on either side; the hinge-line is shorter 
 than the width of the shell, and the cardinal anglesare rounded. The beak in dorsal valve 
 ineurved ; there are faint tracings of the concentric ridges or folds, but, owing to all the 
 specimens being casts, the more delicate markings cannot be determined.” (Etheridge.) 
 In some points there is a close resemblance between S. Strzeleckit and S. Darwinit. 
 
 Loc. and Horizon. Lady Mary Reef, Gympie (The late R. Daintree); No. 6 
 North Phcenix Mine, Gympie (S. Hester)—Gympie Beds ; ? Richards’ Homestead, three 
 miles south-west of Mount Britton Township (&. Hull)—Middle or Marine Series of 
 the Bowen River Coal Field. 
 
 Genus—SPIRIFERINA, D’ Orbigny, 1847. 
 (Comptes Rendus, xxv., p. 268.) 
 SPIRIFERINA DUODECIMCOSTATA, McCoy, Pl. 44, fig. 12. 
 
 Spirifera duodecimeostata, McCoy, Ann. and Mag. Nat. Hist., 1844, xx., p. 234, t. 17, f. 3 and 3. 
 Spirifer duodecimcostata, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 8, p. 234, t. 12, f. 4. 
 
 Obs. The perfectly neat oval form with a well-developed area, simple undivided, 
 rounded, and coarse ribs, to the number of six on each flank, a divided fold, and a 
 
 
 
 
 
 *U.S. Geol. Explor. 40th Parallel, 1877, iv., Pt. 2, p. 255, t. 4, f. 5-8, 
 
235 
 
 simple plain suleus, with the whole crossed by close flat frill-like imbrications, serve to 
 easily distinguish this species. The ribs are divided from one another by their own 
 width apart, but the rib, however, mentioned by McCoy as traversing the sulcus does 
 not appear to be a constant character, for out of eleven specimens before me only two 
 show it. It is a remarkably narrow species, as compared with its width, giving to the 
 marginal outline a rotund or roundedly-triangular appearance. By a lucky coincidence 
 I am happy to be able to show that this shell is referable to Spiriferina rather than to 
 Spirifera. Both in a specimen from Mount Britton, and in another from a New South 
 Wales locality, there is visible the deep central slit left in casts by the median ventral 
 septum, which exists in Spiriferina, as well as the vertical shelly plates. In both 
 examples, also, the punctate shell-structure so characteristic of this genus is quite 
 apparent. The Queensland specimen is by no means perfect, and exhibits only four 
 ribs on each flank. It is an internal cast of the ventral valve, and retains the punctate 
 structure very distinctly. 
 
 Loc. and Horizon. Richards’ Homestead, three miles south-west of Mount 
 Britton Township (4. Z. Morisset; Australian Museum Colln.)—Middle or Marine 
 Series of the Bowen River Coal Field. 
 
 SPIRIFERINA, sp. ind. 
 
 Obs. A small shell occurs in the Star River Series having an entire mesial fold, 
 and indications of numerous concentric, close-set, and frill-like lamella. Seven or eight 
 pronounced ribs were seen on each side the fold, and traces of asperities representing 
 punctate shell-structure. It is probably a small species of Spiriferina. 
 
 Loc. and Horizon. Corner Creek, Great Star River (2. L. Jack)—Star Beds. 
 
 Genus —RETICULARIA, McCoy, 1844: 
 (Synop. Carb, Limest. Foss. Ireland, p. 193.) 
 
 RETICULARIA LINEATA, Martin, sp. ? 
 
 Conch. (Anomites) lineatus, Martin, Pet. Derb., 1809, t. 36, f. 3. 
 Reticularia lineata, McCoy, Synop. Carb. Limest. Foss. Ireland, 1844, p. 198, t. 19, f. 15. 
 Spirtfera lineata, Davidson, Mon. Brit. Carb. Brach., 1858, Pt. 2, p. 62. 
 Reticularia lineata, Davidson, Mon. Brit. Sil. Brach. Suppl., 1882, Pt. 1, p. 81. 
 ap af Waagen, Pal. Ind. (Salt Range Foss.), 1883, Ser. xii., Vol. 1, No. 4, fase. 2, p. 540, t. 42, 
 f, 6-8. 
 
 Obs. This, the type species of McCoy’s genus Reticularia, is represented 
 in Mr. De Vis’ Collection by a portion of a ventral valve only, but possessing the 
 distinctly imbricated lamine and numerous scars of the characteristic double spines. 
 In the face of such features I cannot do less than refer the fragment to this species. 
 A far better example of the ventral valve comes from the Rockhampton District,* and 
 well exhibits the points referred to. They will, at any rate, tend to show the existence 
 of this group of the Spiriferide in the Permo-Carboniferous rocks of Queensland, a fact 
 borne out by the species following. 
 
 Loc. and Horizon. Rockhampton District * (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 Rericutarta Urner, Fleming, sp. 
 Spirifer Urei, Fleming, Brit. Animals, 1828, p. 376. 
 
 Spirifera Urei, Davidson, Mon. Brit. Carb. Brach., 1858, Pt. 2, p. 58, t. 12, f. 13 and 14. 
 Reticularia Urei, Davidson, Mon. Brit. Sil. Brach. Suppl., 1882, Pt. i., p. 81. 
 
 Obs. Casts are met with in the Star River Beds which are difficult to distinguish 
 from those of Spirifera Urei, and more especially the Devonian variety wngwiculus, 
 
 * See note, p. 199. 
 
236 
 
 Phillips. In all the specimens the prominent and projecting umbone of the ventral 
 valve is deeply channelled by a well-marked mesial sinus, which extends far up on the 
 umbone. The latter was tolerably high, but did not overhang the area in any of the 
 specimens. The deep suleation of the ventral valve accords better with the Devonian 
 than the Carboniferous variety of Spirifera Urei, and after a comparison with specimens 
 from both formations, this has been found to be a constant and well-marked character. 
 Loc. and Horizon. Corner Creek, Great Star River (&. L. Jack)—Star Beds. 
 
 Genus—MARTINTIA, McCoy, 1844. 
 
 Martinia, McCoy, Synop. Carb. Limest. Foss. Ireland, 1844, p. 128. 
 re Davidson, Mon. Brit. Carb. Brach., 1884, v., Pt. 3, p. 373. 
 
 MAnrtInia ? PRODUCTOIDES, sp. nov., Pl. 11, figs. 6-11. 
 
 Sp. Char. Shell elongately ovoid, narrow, more or less productiform in outline. 
 Ventral valve elongate, narrow, moderately convex and curved, with a faint sinus in the 
 umbonal region, more apparent in the young state; umbo well incurved over the area, 
 which is short, wide, and somewhat concave, with a wide, deep, triangular fissure. Dorsal 
 valve transversely ovoid, flatter and less arched than the ventral, umbo much less 
 incurved, hinge-line longer in comparison to the width of the shell than in the ventral 
 valve, area broad and concave, with a wide triangular fissure; fold divided by a groove 
 or depression throughout its entire length. Surface of both valves apparently quite 
 smooth. Internal cast of the ventral valve with several longitudinal ridges. 
 
 Obs. Although to some extent related to Martinia glabra, the elongated, 
 produced, and narrow form, and short hinge-line are obviously so different from those 
 characters in that species that I have not hesitated to propose the above name for the 
 present shells, especially as the characters are constant throughout a large number of 
 individuals. I believe them to bea very peculiar form of Jlartinia, possessing less the 
 appearance of that genus, and more that of some Producti, or even abnormal, smooth 
 Pentamert. The curvature of the shell is in itself peculiar, and when viewed from the’ 
 front of the ventral valve has much the appearance of a Productus, but the presence 
 of the well-developed area and fissure at once distinguishes these shells from the genus 
 named. 
 
 Iam undecided whether to regard the valve described above as the dorsal, as such, 
 oras the young condition of the ventral valve. The occurrence of the two in common, and 
 the size and shape of the smaller valves would favour the first view. On the other hand 
 the area and fissure are too well developed to be those of a dorsal valve, and tend to 
 support the latter opinion. 
 
 Loe. and Horizon. Township at Cania Diggings, Burnett; Three Moon Creek, 
 three miles above Cania Diggings (W. H. Rands)—Gympie Beds. At the Training 
 Wall Quarries, Rockhampton, and at Stony Creek, Stanwell [Gympie Beds], internal 
 casts occur, which I believe to be those of this species (The late James Smith). 
 
 Genus—MARTINIOPSIS, Waagen, 1883. 
 (Pal. Indica (Salt Range Foss.), Ser. xiii., Vol. i., Pt. 4, fas. 2, p. 524.) 
 Obs. Prof. J. D. Dana was the first who referred * Spirifer subradiatus, 
 G. B. Sowerby, to the characteristic European species, Spirifera glabra, Martin, a 
 reference afterwards more fully carried out by Prof. De Koninck.+ On the strength 
 
 
 
 * Geology Wilkes’ U. S. Explor. Exped., Vol. x., p. 683. 
 + Foss, Pal. Nouv,-Galles du Sud, 1877, Pt. 3, p. 227. 
 
237 
 
 of the united opinion of these distinguished Paleontologists, I so placed this species in 
 my “Catalogue of Australian Fossils.” A subsequent examination of good internal 
 casts, however, of Morris’s species, shook my belief in the advisability of this step, a 
 belief still further strengthened on reading Dr. Waagen’s description of his genus 
 Martiniopsis. 
 
 If Spirifer subradiatus, which is, without doubt, one of the most characteristic 
 shells of portions of our Permo-Carboniferous deposits, is rightly placed by Messrs. 
 Dana and De Koninck, it naturally falls into Wartinia, McCoy, a genus now universally 
 adopted for shells after the type of Spirifera glabra, Martin. 
 
 Following Waagen, Martinia and his Martiniopsis are thus distinguished :— 
 
 
 
 
 
 
 
 
 
 
 
 
 
 Area in d. Dental plates Septal plates Area in y. 5 
 Panties | valve. in v. valve. in d. valve. valve. Sheer SerBCourel 
 | 
 Martinia cs soe absent ...} absent... | large ... | moderately punctate. 
 Martiniopsis ... a present ...| present ...| present... | sinall ... | punctate-fibrous. 
 
 
 
 
 
 “¢ By the smoothness of the shell, and the general appearance, the forms belonging 
 to this genus,” says Waagen, when describing Martiniopsis, “appear to be very closely 
 related to Martinia, and I was for a long time inclined to place these shells in that 
 genus ; but, after a careful study of typical specimens of Martinia glabra from Visé, 
 which I owe to the kindness of Mons. De Koninck, I found that these shells were 
 devoid of dental, as well as of septal plates, and were therefore distinct generically 
 from the Indian fossils ”»—7.e., Martiniopsis. 
 
 Presuming on the accuracy of Waagen’s discovery in the structure of Martinia 
 glabra, it necessarily follows that we have two outwardly similar types of the non- 
 costate Spirifers, possessing a widely different internal structure — Martinia and 
 Martiniopsis. 
 
 Referring to Australian members of this family exhibiting this outward appear- 
 ance, Waagen says—‘ In Australia the genus” (Martiniopsis) “appears to have attained 
 a somewhat more extensive development. It seems at least. probable that species like 
 Spir. Darwinii, Spir. oviformis, and the large form figured by Mons. De Koninck under 
 the name of Spir. glaber, belong to the present genus.” 
 
 With the view of following out this suggestion, I have assembled a large number 
 of internal casts of Spirifera subradiata, Morris, both from New South Wales and 
 Queensland localities, and also Spirifera Darwinii, Morris (non De Koninck), aud I find 
 them to possess the leading characters of Murtiniopsis, as laid down by Waagen, in all 
 but one trivial feature. Taking Spirifera subradiata as the type, by reproducing from 
 internal casts the aspect of the shelly plates in some yielding and suitable material, it 
 will be found that very strong dental plates exist in the ventral valve. In casts these 
 produce the deep depressions on each side the umbonal projection, and terminating, 
 under the hinge-line, in the thick teeth. In the dorsal valve similar septal, or crural 
 plates produce like slits or depressions, and terminate under the hinge-line in sockets 
 for the reception of the above teeth. It further becomes apparent, from a study of these 
 internal casts, that the dorsal valve possessed a small area. 
 
 The presence of these shelly plates will at once remove Spirifera subradiata from 
 the genus Martinia to Martiniopsis, under the name of Martiniopsis subradiata, Morris, 
 sp., and it will cease to be a synonym of Martinia glabra, Martin, sp. The internal 
 structure of this species was not lost sight of, to some extent, by De Koninck, but he 
 failed to appreciate its importance. 
 
238 
 
 According to Waagen the shell structure of both Martinia and Martiniopsis is 
 punctate. In I. subradiata some of the shelly layers are certainly punctate, others 
 equally fibrous. This is shown on one of Mr. De Vis’ specimens, and I have seen a 
 similar appearance on New South Wales examples. I should be inclined to regard it as 
 punctate-fibrous; some portions of the shell are undoubtedly fibrous, this structure 
 having been first noticed by Dana,* whilst the punctate condition was equally elicited 
 by De Koninck. 
 
 It must be distinctly understood that in thus adopting Martiniopsis, as separated 
 from Martinia, I have relied solely on Waagen’s description of the structure of the 
 latter. I very much wished to obtain specimens of Martinia glabra, to examine the 
 internal structure for myself, but circumstances have prevented this. However, the 
 general accuracy of Dr. Waagen’s observations emboldens me to place our Australian 
 form provisionally in his genus, leaving to others who may have a plenitude of Martinia 
 glabra to settle this question finally. 
 
 Types. Martiniopsis inflata, Waagen (Indian) ; Martiniopsis subradiata, Morris, 
 sp. (Australian). 
 
 Manrrtiniopsts suBRADIATA, G. B. Sowerby, sp., Pl. 11, fig. 14. 
 
 Spirifera subradiata, G. B. Sowerby, Darwin’s Geol. Obs. Vole. Islands, 1844, p. 159. 
 Spirifer subradiatus, Morris, Strzelecki’s Phys. Descrip. N. 8. Wales, &c., 1845, p. 281, t. 15, f. 5, t. 16, f. 1-4, 
 »,  glaber, Dana (non Martin), Geology Wilkes’ U. 8, Explor. Exped., 1849, Vol. x., p. 688, Atlas, 
 re lbetilty 
 na We Kentnek (non Martin), Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 227 (excel. syn.), t. 
 TOES toh hale h ih Meh oi, diver. 
 »,  Darwini, De Koninck (non Morris), Ibid., p. 230 (excl. syn.), t. 10, f. Lla-b, t. 11, f. 10-10a, t. 16, 
 Vie dle 
 Spirifera glabra, Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 280. 
 
 Sp. Char. Shell variable in shape and proportions, but usually transversely oval, 
 at times becoming very transverse, and both valves much compressed; or short and 
 oval, with the valves almost equally convex. Hinge-line less than the width of the shell, 
 with the alar angles always rounded. Area of the ventral valve wide and irregular, but 
 in the dorsal valve, narrow, and much longer. Ventral umbo either depressed and 
 channelled, or to some extent elevated, and to all intents and purposes entire, usually 
 overhanging the area. Sinus wide and plain, bounded by prominent obtuse folds; 
 dorsal fold high and undivided, or broad, flattened, and divided by a median depression, 
 and often bounded laterally by a groove on each side. Front margin in very convex 
 forms much sinuated, but in compressed examples more in one plane. Teeth of the 
 ventral valve large and thick; dental plates strong and long; cardinal muscular 
 impressions long and oval, striated longitudinally and divided medianly by a double 
 septum ; ovarian impressions largely developed on the flanks. In the dorsal valve the 
 septal plates are very long, frequently reaching half across the valve ; adductor impres- 
 sions elongately lingual, separated by a septum. Spiral arms highly developed, and 
 nearly filling the interior of the shell. Cardinal process thick and large. The surface 
 of the valves is smooth, with the exception of wide concentric lamine of growth, but one 
 
 or more obtuse radiating folds (as many as four) are sometimes present, according to ° 
 
 the variety. On the surface of the cast, numerous indistinct, or half-effaced radiating, 
 close ridges are faintly visible both on the flanks and dorsal fold, and in the sinus. Shell 
 structure punctate and fibrous. 
 
 Obs. Since Dana first referred Spirifera subradiata, G. B. Sowerby, to Martin’s 
 S. glabra, it has been customary to unite with it a number of shells, all more or less 
 
 
 
 * Geology Wilkes’ U. 8, Explor. Exped., Joc. cit., p, 683. 
 
 o:. 
 
239 
 
 resembling one another, but still differing to some extent in shape, and the exterior 
 markings of the test. No doubt great resemblance exists externally between S. glabra 
 and Martiniopsis subradiata, but, if Dr. Waagen’s observations are to carry any weight, 
 the likeness ceases here. I now purpose selecting a form to serve as the type of I 
 subradiata, and to consider the other conditions as well marked and recognisable varieties. 
 
 The true IZ. subradiata, as represented by Morris’s figures, given in Count de 
 Strzelecki’s Work,* is an elliptical, rather transverse, sub-compressed, comparatively 
 smooth shell, possessing a wide shallow sinus, a low broad fold divided by a median 
 ill-defined groove, and bounded on each side by a similar furrow, a high prominent 
 ventral umbo, and long shoulders on either side. The flanks are either gently convex 
 or flattened, with, now and then, undefined radiating coste, crossed by distant concen- 
 tric lamine of growth. 
 
 This species at times attains a considerable size, one specimen having come under 
 my notice quite three and a-half inches in transverse diameter. Internal casts of the 
 species proper usually display the slits left by the dental plates and processes of the 
 ventral and the septal plates of the dorsal valve, the latter extending into the body of 
 the shell for fully one-third of its depth. Such examples are met with in the Rock- 
 hampton District, especially at Banana Creek. 
 
 The structure of the test, to include this shell in Martiniopsis, should be punctate, 
 and it is so described by De Koninck, who says—‘ Le tét est assez mince et perforé,”’ 
 the perforations being arranged in quineunx. In one of our Queensland specimens, 
 preserved in limestone, a delicate pitting is observable on both flanks. The other portions 
 are covered with a very fine striation or ribbing, visible to the naked eye. Wherever 
 the surface is abraded this striation has the appearance of longitudinal tubes running 
 through the substance of the test ; but on those portions merely smoothed over by the 
 denuding agent, these tubes appear as darker lines traversing the lighter coloured 
 limestone of which the shell is composed. 
 
 The following may be taken as characteristic figures of I. subradiata :— 
 
 Morris in Strzelecki, loc. cit., t. 16, f. 1-4. 
 De Koninck, Joc. cit., t. 12, f. 1. 
 Tab. nost., Pl. 11, fig. 14. 
 
 The varieties of this species known to me are, viz. :— 
 
 1, Var. Morrisii (mihi). See post. 
 
 2. ,, transversa (mihi), De Koninck’s Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, t. 12, f. 10. 
 
 3. ,, Konincki (mihi), De Koninck’s Foss. Pal. Nouy.-Galles du Sud, 1877, Pt. 3, t. 10, f. 11 @ and 8, 
 t. 11, f. 10 and 10a, t. 16, f. 1 (=Spirifera Darwinii, De Kon., non Morris). 
 
 In addition to these varieties, the two last of which I have not seen from ° 
 Queensland, there is another form represented in Pl. 40, fig. 3. At first sight this would 
 seem to be a variety of McCoy’s Spirifera oviformis,+ but it may be only a condition of 
 M. subradiata on which a good deal of oblique lateral pressure has been exerted, and 
 the ventral sulcus much pressed together. 
 
 Martiniopsis subradiata is quite distinct from both the Indian species, and its 
 relation to AZ. Darwinii will be touched on under the description of the latter species. 
 
 Loc. and Horizon. Stonehumpy Creek, Bowen River (#. LZ. Jack); Banauva 
 Creek, near Banana, Dawson River (H. Mackay, Colln. De Vis; and the late James 
 Smith); Richards’ Homestead, three miles south-west of Mount Britton Township 
 (R. Hull)—Middle or Marine Series of the Bowen River Coal Field; Gympie (G. Sweet ; 
 Colln. Sweet, Melbourne)—Gympie Beds. The longitudinally elongated variety is from 
 Banana Creek (H. Mackay ; Colln. De Vis). 
 
 Plex visetion sls 
 + Ann. and Mag. Nat. Hist., 1847, xx., p. 234, t. 13, f. 5 and 6. 
 
240 
 
 MARTINIOPSIS ? SUBRADIATA, var. Mornrisil, var. nov., Pl. 11, figs. 12 and 138. P 
 
 Spirifer subradiatus, Morris in Strzelecki’s Phys. Descrip. N. 8S. Wales, &c., 1845, t. 15, f£.5 (non t 15, 
 f.5 a and d, t. 16, f. 1-4. 
 
 Spirifera glabra, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, t. 12, f. 1, la, t. 11, f. 8 (non 
 t. 12, f. 1b, 1c). 
 
 Var. Char. Shell round-oval, convex, width and height approximately equal, or 
 but very slightly different, hinge- line much shorter than the “width of the shell; ventral 
 area well reseed ventral umbo usually somewhat depressed and channelled! but not 
 greatly incurved ; dorsal fold high, broad, and undivided ; sinus very broad and deep, 
 continuous with the channelling of the umbo, and limited on each side by a prominent 
 obtusely rounded fold; surface quite plain with the exception of growth lamine. 
 
 Obs. I propose to distinguish by the above varietal name those forms of 
 M. subradiata in which the longitudinal measurement is at least equal to the transverse, 
 and at times exceeds it, giving rise to an oval outline. Such a variety is represented 
 by the figure of Morris above quoted. ‘This shape is accompanied by a very pronounced 
 fold and sinus, the former being limited laterally by a depression and corresponding 
 fold on each side, and the latter by bounding obtuse ridges, or folds. The true 
 MW. subradiata is much wider than high, as expressed by Mr. G. B. Sf tad who says, 
 ‘The breadth of this shell is rather greater than its length.” 
 
 A very closely allied shell, so far as external appearance goes, is Spirifera 
 hombronianus,t D’Orb., in which the umbo is erooved, even quite to the apex of 
 the beak. 
 
 At times this variety assumes one or two other rib-like folds in addition to 
 those bounding the fold and sinus. I have seen one example with three ribs on each 
 flank, and three others with two. An additional one is visible in Morris’s figure. 
 
 Loe. and Horizon. Spring Creek, Cania, Burnett (W. H. Rands)—Gympie 
 Beds. 
 
 Martintorsis Darwintt, Morris, sp. 
 Pl. 9, figs. 13 and 14; Pl. 39, figs. 5-7. 
 
 Spirifer Darwinii, Morris, Strzelecki’s Phys. Descrip. N. S. Wales, 1845, p. 279 (non De Koninck). 
 5,  subradiatus, Morris, loc. cit., t. 15, f. 5a (fig. eact exclusis—non G. B. Sowerby). 
 »  Darwinii, Dana, Geology Wilkes’ U. 8. Explor, Exped., 1849, Vol. x., p. 684, Atlas, t. 1, f. 7. 
 »  Darwinti, Etheridge fil., Proc. R. Phys. Soc. Edinb. 1880, v., p. 281, t. 7, ff. 7-10, t. 8, f. 11. 
 
 Sp. Char. 'Transversely ovoid, very convex, gibbous and deep, with the valves 
 equally convex; hinge-line very short, much less than the width of the shell; alar 
 . angles regularly rounded; alar expansion, or lateral portions of the shell, short, 
 rounded, and attenuating but little outwards; front margin deeply sinuated. Ventral 
 valve convex, depressed from above in the umbonal region, with a very deep, broad, and 
 pronounced sinus, plain and without subdivisions of any kind; cardinal process 
 depressed, not high, quite horizontal ; umbo but little incurved; area short and broad. 
 Dorsal valve very convex in the middle line, quite “ pigeon-breasted,” with a high, much 
 pinched up, and very straight-sided fold, horizontal in the umbonal region, projecting 
 to the front sometimes far beyond the lateral front edges of the valves, and subdivided 
 in casts for about half its length by a narrow slit, indicating the presence of a thin 
 septum ; area smali. The dental processes, and their extensions in the ventral valve, 
 are very thick, almost completely surrounding the muscular impressions; the latter 
 deeply excavated, and lingual in outline, convex medianly. The septal processes of 
 the dorsal valve are very thick and short; combined muscular impressions almost 
 
 
 
 * Darwin’s Geol. Obs. Vole. Islands, 1844, p. 159. 
 + Dumont D’Urville’s Voy. au Péle Sud, Geol. Atlas, t. 6, ff, 15-18, 
 
241 
 
 confined to the ridge, or the fold. Surface of the valves plain, but the fold and sinus 
 are sometimes followed by one, two, three, or even four sharp, well-separated, radiating 
 costx on each side, at times well marked, at others very faint and indistinct ; the inter- 
 spaces between these cost are always much wider than the latter, wlulst on the dorsal 
 valve the fold is followed by a deep valley on each side. 
 
 Obs. In this species, as in the former, I have had the advantage of studying both 
 good internal casts and examples with the test preserved. If Spirifera subradiata, 
 G. B. Sby., is correctly placed in Martiniopsis, the present species will also fall into that 
 genus, as their internal structure is on the same general plan. The chief points of 
 interest in I. Darwinii are the very convex, deep, and equal valves, large fold, and 
 highly pinched-up sinus ; but above all the strange horizontal truncature of the umbonal 
 regions of both valves, giving to the shell a square-topped or “ pigeon-breasted’’ 
 appearance, the truncated cardinal process and the fold of the dorsal valve forming, by 
 their imaginary union, almost a right angle. It is this feature, with the marked 
 convexity of the valves, which serves to distinguish IZ, Darwinii from MW. subradiata. 
 
 I am quite in accord with Prof. De Koninck in referring one of the shells 
 figured by Professor Morris as Spirifera subradiata, G. B. Sowerby, to the present 
 species, after comparison with Morris’s type.* In justice to Prof. Morris, it must be 
 borne in mind that he himself hinted at this union. Beyond this, however, I cannot go 
 with this much-lamented and distinguished Palxontologist in his interpretation of 
 Spirifera Darwinit. To me all his figures of this species represent but a variety of 
 Martiniopsis subradiata, to which on a previous page I have ventured to apply the 
 varietal name of Konineki. Morris but very briefly described his 8. Darwinii, and did 
 not ostensibly figure it. In the description, my former Master refers to the equally 
 convex valves, and says—‘‘It is a very neat shell, and presents some resemblance to one 
 of the varieties of 8. swbradiatus (Pl. xv., fig. 5a).’’ | This so-called variety I take to be 
 the veritable S. Darwinii of Morris, because the shell in question does not correspond 
 at all with WZ. subradiata, but possesses peculiar features of its own. An examination 
 of the figure quoted will show how widely it differs from any illustrations of the last- 
 named species, whether those of Morris or De Koninck; and no better term could have 
 been employed in its description than that of ‘neat.’ Compare the elegantly alate 
 appearance of the sides possessed by “ PI. xv., fig. 5a,” with the gradually compressed 
 and elongated ends of the figures given by Morris of the Spirifera subradiata. 
 
 The muscular scars in the ventral valve are lingual, and in casts very prominent, 
 the surface more or less hollowed or concave. In the dorsal valve the impressions are 
 almost confined to the apex of the fold, and are separated by a septum. 
 
 A good deal of variation occurs in the radiating coste of the exterior. In some 
 individuals there is a single and indistinct rib, in others one well marked and another 
 faint, or they become more numerous as described above. 
 
 The internal processes project much less into the interior of the shell than do 
 those of I. subradiata, and, although quite as large, produce shallower impressions in casts. 
 
 At Yatton, there appears to be a variety of this species Jiffering from the species 
 proper in having the ribs closer, rounded, and rather curved, but this is accompanied 
 by the peculiarities of the cardinal process mentioned above. 
 
 Loc. and Horizons. Coral Creek, Bowen River, below Sonoma Road- 
 crossing (Rt. L. Jack); Parrot Creek, Bowen River, four and a-quarter miles up (2. L. 
 Jack) ; Richards’ Homestead, three miles south-west of Mount Britton Township, 
 (A. L. Morisset)—Middle or Marine Series of the Bowen River Coal Field; Yatton 
 Gold Field (&. L. Jack)—Gympie Beds. 
 
 * Strzelecki’s Phys, Descrip. N. 8S. Wales, &c., 1845, t, 15, f. 5a. 
 
 
 
 
 
 Q - 
 
242 
 Family—NUCLEOSPIRID@. 
 
 Genus—RETZIA, King, 1850. 
 (Mon. Permian Foss. England, p. 187.) 
 
 RETZIA RADIALIS, Phillips, sp., Pl. 11, figs. 24 and 25. 
 Terebratula radialis, Phillips, Ill. Geol. Yorksh., 1836, Pt. 2, p. 228, t. 12, f. 40 and 41, 
 Retzia radialis, Davidson, Mon. Brit. Carb. Brach., 1860, Pt. 3, p. 87, t. 17, f. 19-21. 
 
 Obs. Numerous examples of a small Brachiopod, always in the form of casts, 
 with a highly punctate structure, and radiating ribs, are to be met with in the Star 
 Beds, usually compressed almost flat, and sometimes obliquely distorted. The radiating 
 coste appear to be about fourteen or fifteen in number, angular, sharp, and prominent, 
 which, with the valleys between, are densely sprinkled with rugosities representing the 
 very fine punctations of the shell. 
 
 The ribs ornamenting the valves are much too numerous for the Devonian Retzia 
 ferita, Von Buch, and still more so for the Carboniferous R. wlotriv, De Koninck, in 
 which there are only from seven to nine, and very prominent, giving a much bolder 
 appearance than that possessed by the Corner Creek shell. It is with Retzia radialis, 
 Phillips, that the greatest resemblance exists, both in size, number of the coste (eleven 
 to twenty-three), and probably also in shape. So far as I am aware, only one species 
 of Retzia has hitherto been described from Australian rocks, and that a Silurian species, 
 viz., R. Saltert, Davidson, by Prof. De Koninck. The occurrence of another species in 
 North Australia is therefore an interesting fact. 
 
 Loc. and Horizon. Corner Creek, Great Star River (2. L. Jack)—Star Beds. 
 
 ReEtzr1a ? LILYMERENSIS, sp. nov., Pl. 11, figs. 20-22. 
 
 Sp. Char. Shell elongately deltoid, attenuated or narrow towards the beaks, and 
 expanded towards the front; valves equally convex at a point drawn through them 
 immediately below the beak of the dorsal valve, thence rapidly decreasing towards the 
 front margin, which is very wedge-like; umbo of the ventral valve moderately large 
 (its apex broken), and probably overhanging that of the dorsal valve but little; surface 
 of both valves covered with close, equal, simple and rounded coste, [shell structure 
 punctate P]. 
 
 Obs. The reference of this shell to Refzza is provisional only, the nature of the 
 interior being quite unknown. It possesses much the outward appearance of a Retzia, 
 but repeated and close examination has quite failed to detect perforation of the shelly 
 matter with any degree of certainty. 
 
 In form, &. ? lilymerensis is very like some of the genera figured by Dr. W. 
 Waagen from the Productus Limestone of the Salt Range, Hindostan, such, for instance, 
 as Hemiptychina, Waagen,* and Dielasmina and Notothyris, Waagen,t but without 
 possessing the forward plice or ribs of these genera. Could I have satisfactorily shown 
 the presence of a punctate shell structure in the present species, it might very justifiably 
 have been referred to Dielasmina, as the three septal plates visible on the umbonal 
 surface of the dorsal valve, in both shells, closely correspond. Although the Australian 
 shell is not coarsely plicate, it bears a large number of smaller coste, which certainly do 
 become larger and coarser towards the front margin, after the manner of Waagen’s 
 genus. 
 
 
 
 * Pal. Indica (Salt Range Fossils), 1882, Ser. xiii., Vol. i., No. 4, fase. 1, p. 361, 
 + Ibid., p. 359, , 
 
243 
 
 In external appearance, our shell equally resembles the genus Acambona, C. A. 
 White,* but here again a want of knowledge of its internal characters, and the apparent 
 absence of a punctate test, preclude any definite reference. 
 
 The only Australian fossil having any resemblance to R. ? lilymerensis is Atrypa 
 pliecatella, De Koninck,+ from the so-called Lower Devonian of New South Wales, 
 which has a similar sculpture, but is very much less deltoid and attenuated towards the 
 umbones. 
 
 Loc. and Horizon. Blenayon, Lilymere, near Rockhampton (The late James 
 Smith) —Gympie Beds. 
 
 
 
 Family—ATHY RID. 
 
 Genus—ATHY RIS, McCoy, 1844. 
 (Synop. Carb. Limest. Foss. Ireland, p. 146.) 
 
 Atuynris Roysi1, Leveillé, sp., Pl. 11, fig. 15. 
 Spirifer Roysti, Leveillé, Mém. Soc. Geol. France, 1835, ii., p. 39, t. 2, f. 18-20. 
 Athyris Roysti, Davidson, Mon. Brit. Carb. Brach., 1858, Pt. 2, p. 84, t. 18, f. 1-11 (for synonymy). 
 
 Obs. Two crushed examples, not to be distinguished from this widely distributed 
 shell, were obtained by the late Mr. James Smith, with the characteristic spines 
 exposed as a frill around the margin of the valves, each separate from its neighbour, a 
 character which at once separates 4. Roysii from the allied 4. planosulcata. The shell 
 figured by Prof. De Koninck ¢ under the latter name does not, as portrayed, exhibit, to 
 my mind, the slightest resemblance to the species in question. The difficulty of 
 correct identification is further increased by the careless manner in which the references 
 in the text are made to the figures on the plates, a fault which more or less pervades 
 the whole work. Through this, it is at times difficult to understand to which figure the 
 Professor is referring in his descriptions. 
 
 Jn the Cawarral Serpentine Mr. Smith found the impression of a Brachiopod, 
 which is either a perforate Spirifera of the group Reticularia, or an Athyris, probably 
 the latter. 
 
 Loc. and Horizon. Stony Creek, Stanwell, near Rockhampton (Lhe late James 
 Smith) —Gympie Beds. 
 
 ATHYRIS AMBIGUA, J. de C. Sowerby, sp. 
 Spirifer ambiguus, J. de C. Sowerby, Min. Con., 1822, iv., p. 105, t. 376. 
 Athyris ambigua, Davidson, Mon. Brit. Carb. Brach., 1858, Pt. 2, p. 77, t. 15, f. 16-22 (for synonymy) 
 
 Obs. A crushed, but at the same time readily recognisable specimen of this 
 equally characteristic shell has been found by Mr. W. H. Rands. Although only a cast 
 the suleus of the ventral valve is still traceable, and there are indistinct remains of 
 concentric ornamental lines of growth. 
 
 Loc. and Horizon. Hawkins’ Gully, Kariboe Creek, Kroombit Diggings, Port 
 Curtis (W. H. Rands)—Gympie Beds. 
 
 ArHyris Ranpst, sp. nov., Pl. 11, figs. 16-18. 
 
 Sp. Char. Shell obovoid, gibbous, ball-like; valves almost equally convex; ventral 
 valve very convex, the umbo but little elevated; sinus imperfectly visible on the body 
 of the valve, but broad towards the front. Dorsal valve convex and gibbous, especially 
 
 
 
 * Proc. Boston Soc. Nat. Hist., 1862, ix., p. 27 (fide De Koninck, Faune Cale. Carb. Belgique, 1887, 
 Pt. 6, p. 96). 
 
 + Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, t. 3, f. 4 and 4a, 
 
 t+ Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, t. 9, f. 6, 
 
 ? 
 
244: 
 
 about the umbonal region, with a prominent and elevated, but rounded fold, rendering 
 the shell more or less trilobed. Front margin sinuated, much elevated medianly and 
 depressed laterally. Foramen small, and contiguous to the dorsal valve. Surface very 
 plainly concentrically lined, and rather strongly radiately striated (? spine bases). 
 
 Ots. This species appears to be nearly related to Athyris subtilita, Hall,* which 
 is described as possessing “faint, often almost imperceptible, radiating strie.” In the 
 present species the strie, if they be so, and-not spine bases, are much too coarse to 
 come within this definition. It certainly agrees better with the American shell than it 
 does with the form described by Dr. Abich as Athyris (Spirigera) protea, var. subtilita, 
 Hall, from the Carboniferous rocks of Armenia.t Athyris globularis, Phill., is another 
 shell with which the present may be compared in a general way. 
 
 Loc. and Horizon. Uawkins’ Gully, Kariboe Creek, Kroombit Diggings, Port 
 Curtis (W. H. Rands)—Gympie Beds. 
 
 Family—RHYNCHONELLID. 
 Genus—RHYNCHONELLA, Fischer, 1809. 
 
 (Notice Foss. Gouv. Moscou, p. 35.) 
 
 RuHYNCHONELLA PLEURODON, Phillips, sp., Pl. 11, fig. 23. 
 
 Terebratula pleurodon, Phill., Ill. Geol. Yorksh., 1836, Pt. 2, p. 222, t. 12, f. 25-80 (non 16). 
 Rhynchonella pleurodon, Davidson, Mon. Brit. Carb. Brach., 1860, Pt. 3, pp. 101 and 246, t. 23, f. 1-15, 
 16-22 2, 
 nn *y De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 219, t. 9, f. 4-4e. 
 
 Obs. A number of decorticated impressions, resembling Rhynchonella pleurodon, 
 occur on the surfaces of blocks from Stanwell, associated with Chonetes, Productus, and 
 other shells. It is the variety with three or four ribs in the sulcus, and the fold much 
 produced forward. In the dorsal valve the flanks each carry four ribs. 
 
 Loc. and Horizon. Stony Creek, Stanwell, near Rockhampton (The late 
 James Smith)—Gympie Beds ; Gully rising in cliff between two peaks of a mountain, on 
 left bank of Keelbottom River, north of Old Plum-tree Inn (&. ZL. Jack)—Star Beds. 
 
 RHYNCHONELLA, sp. ind. 
 
 Obs. A single small shell, ovately trigonal in shape, with a small sharp beak, 
 small convexity of valves, and the dorsal valve bearing twelve angular ribs, simple and 
 without imbricating strie. It is not unlike a Refzia, but the shell substance is 
 impunctate. It might pass for a small variety of Rhynchonella pleurodon, but the 
 dorsal valve is rather too flattened in the middle line. ; 
 
 Loc. and Horizon. Township, Cania Diggings, Burnett (W. H. Rands)— 
 Gympie Beds. 
 
 Family—ORTHID. 
 Genus—ORTHIS, Dalman, 1828. 
 (Kongl. Vet. Acad. Handlingar, 1827 [1828], p. 96.) 
 
 ORTHIS RESUPINATA, Martin, sp., Pl. 11, figs. 26 and 28. 
 Orthis resupinata (Martin), Davidson, Mon. Brit. Carb. Brach., 1861, Pt. 4, p. 180, t. 29, f. 1-6, t. 0, f. 1-5. 
 
 Obs. Internal casts of this cosmopolitan species, in a good state of preservation, 
 are to be found in the Star River Beds, of all sizes up to one and a-half inches in 
 breadth. They resemble the small forms figured by Mr. Davidson from Millicent,* in 
 
 i Stanbury’s Exped. Valley Gt. Salt Lake of Utah, 1852, App. E, p. 409. 
 + Geol. Forschungen in den Kaukasischen Liindern, 1878, t. 8, f. 10-12, 
 
245 
 
 Ireland, even to the broad sulcus in the front part of the ventral valve. A few of the 
 specimens are rounder and deeper, and approach the figure given by the same Author of 
 examples from Yorkshire.t A few external impressions have also been obtained, in 
 some of which I believe it is possible to trace the characteristic spines. The largest 
 specimens, however, both external impressions and internal casts, have been collected by 
 the late Mr. James Smith, at Stanwell. 
 
 Prof. L. G. De Koninck united Orthis australis, McCoy, with this species, and in 
 this I followed him in the “ Catalogue of Australian Fossils.’ But on looking into the 
 matter again it seems to me that a good deal may be said for the separate retention of 
 the latter as a species. By its general outline and form, O. australis appears to be a 
 much nearer ally of Orthis Michelini. 
 
 Loc. and Horizon. Corner Creek, Great Star River (R. ZL. Jack and P. W. 
 Pears)—Star Beds ; Stony Creek, Stanwell, near Rockhampton (The late James Smith) ; 
 Gracemere Ridges, Stanwell, near Rockhampton (A. F. Wood)? ; Athelstane Range, 
 Rockhampton (The late James Smith) ; Hawkins’ Gully, Kariboe Creek, Kroombit 
 Diggings, Port Curtis (W. H. Rands)—Gympie Beds. 
 
 OrTHIs AUSTRALIS, McCoy, Pl. 11, figs. 27 and 29. 
 Orthis australis, McCoy, Ann. and Mag. Nat. Hist., 1847, xx., p. 234, t. 13, f. 4 and 4a, 
 
 Obs. Internal casts and external impressions have been collected in the 
 Rockhampton District both by Mr. C. W. De Vis and the late Mr. James Smith. Some of 
 these closely resembled Orthis Michelini, Leveillé,t but differed from this well-known 
 European species in possessing porportionately longer, narrower, and more reniform 
 cardinal muscular impressions. In addition to this, the adductor impressions were also 
 much smaller. I think there can be little doubt, however, that O. australis, McCoy, is 
 the representative of the other species in Australian rocks. The adductor impressions 
 are simple, as in Orthis resupinata, but more heart-shaped, and not double as in 
 O. Michelini, but beyond this the only other points of difference are those stated above. 
 The pedicle scar is strong and well marked (Pl. 11, fig. 29), but the ovarian impressions 
 are not apparent; and, lastly, the dental plates are certainly longer for the size of the 
 
 shell than in O. Michelini. 
 Loc. and Horizon. Stony Creek, Stanwell (Lhe late James Smith)—Rockhampton 
 
 District ; § (C. W. De Vis ; Colln. De Vis)—Gympie Beds. 
 
 Family—STROPHOMENID. 
 
 Genus—STROPHOMENA (Rafinesque, 1820), Blainville, 1824. 
 (Dict. Sci. Nat., xxxii., p. 302.) 
 
 STROPHOMENA RHOMBOIDALIS, var, ANALOGA, Phillips. 
 Pl. 12, figs. 8 and 9; Pl. 40, fig. 6. 
 Producta analoga, Phillips, Ill. Geol. Yorksh., 1836, Pt. 2, p. 215, t. 7, f. 10. 
 Strophomena rhomboidalis, var. analoga, Davidson, Mon. Brit Carb. Brach., 1860, Pt. 3, p. 119, t. 28, f. 1-18 
 (for general synonymy). 
 Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., pp. 331 and 333 
 Ue diane, Cichatelllay ys tals sea us lst 
 7 99 Etheridge fil., Cat. Australian Fossils, 1878, p. 60. 
 Obs. This shell occursin the Silurian, Devonian, and Carboniferous rocks over 
 
 large areas of the globe, and abundantly in the Permo-Carboniferous Series of the 
 
 9 99 ”» 
 
 * Mon. Brit. Carb. Brach., 1861, Pt. iv., t. 30, f. 1. 
 + Ibid,, t. 30, f. 3. 
 
 + Mem. Soc. Géol. France, 1835, ii., p. 39. 
 
 § See note, p. 199, 
 
246 
 
 Gympie gold-bearing beds. The latter differs in no respect from the well-known forms 
 described by Wahlenberg, Sowerby, Phillips, De Koninck, and Etheridge. 
 
 The later collections of my Colleague contain a few examples of this variety 
 exhibiting its character in a more satisfactory manner than those obtained by the late 
 Mr. Daintree, as, for instance, one specimen in which the vertical smooth front of the 
 shell is visible. A single individual was likewise obtained from the Great Star Beds—a 
 small dorsal valve exhibiting the characteristic transversely corrugated surface. Some 
 very interesting examples of this protean species are in the Queensland Museum, both 
 internal casts and examples retaining a large proportion of shelly matter, with the 
 corrugations on the visceral surface, general fine strie, and bold vertical front fully 
 preserved. One cast of the interior exhibits, not only the muscular impressions, but 
 also the vascular system. 
 
 Loc. and Horizon. Lady Mary Reef, Gympie (The late R. Daintree); Gympie 
 (R. L. Jack) ; Rockhampton District * (C. W. De Vis ; Colln. De Vis)— ‘Gympie Beds ; 
 Corner Creek, Great Star River (R. LZ. Jack)—Star Beds. 
 
 Genus—DERBYIA, Waagen, 1884. 
 (Pal. Indica. (Salt Range Fossils), Ser. xiii., Vol. iv., fas. 3, p. 591.) 
 
 DerByia SENILIS, Phillips, sp., Pl. 12, figs. 1-6. 
 Spirifer senilis, Phill., Ill. Geol. Yorksh., 1836, ii., p. 216, t. 9, f. 5. 
 Streptorhynchus crenistria, var. senilis, Davidson, Mon. Brit. Carb. Brach., 1861, Pt. 4, t. 27, f. 2-7. 
 Lepteena senilis, McCoy, Brit. Pal, Foss., 1853, fas. 3, p. 45a, 
 Orthatetes crenistria, var. senilis, Etheridge fil., Proc. R. Phys. Soc, Edinb., 1880, v., p. 282, t. 8, 
 f. 12-15. 
 Derbyia senilis, Waagen, loc. cit., p. 593. 
 
 Obs. Accepting Dr. W. Waagen’s separation of the genera Streptorhynchus 
 and Orthotetes, and the redistribution of species between them and his new genus 
 Derbyia, it is at once apparent that the Australian shell I have described as O. 
 erenistria, var. senilis, will fall into the last-named, and regain its specific position as 
 originally described by Phillips. It appears to me to have a much greater affinity 
 with the British shells than with any of those described from the Carboniferous Beds of 
 the Indian Salt Range Series by Dr. Waagen. 
 
 The Queensland specimens have, in common with British examples, the semi-conic 
 ventral valve, with step-like interruptions “ produced by two or three very large and 
 irregular concentric undulations,’ the elevated, but not incurved beak, and the wide 
 area with its convex deltidium. Similarly, the dorsal valve exhibits the straight hinge- 
 line, evenly convex surface, and much less marked undulations. The striation of the 
 valve likewise appears to be identical, and there are also the same concentric laminations 
 of the area and deltidium as seen in some British examples. Dr. Waagen, in defining 
 Derbyia, says nothing about the punctate nature of the shell, but in the present 
 examples the shelly matter is decidedly and distinctly punctate, and when the surface 
 is at all worn the puncte are everywhere visible, and more especially on the area. I 
 believe the punctate structure of the shell in Orthotetes and Streptorhynchus has not 
 been generally recognised, for in the generic descriptions given by all the best authors 
 the shell is said to be impunctate. However, that most accurate observer, Professor W. 
 King, has not omitted to notice this peculiarity in the Permian species Streptorhynchus 
 pelargonatus, Schlotheim.s Mr. Davidson has also seen the same structure in some 
 British Orthotetes. 
 
 * See note, p. 199. 
 + Mon, Permian Foss, England, 1858, p. 109. 
 
24.7 
 
 The puncte on the exterior of the shells appear as small rugosities scattered at 
 random over the surface of the ribs or striew, and intervening valleys, ornamenting these 
 shells, but when worn to any extent their perforate character at once becomes apparent. 
 They are, in particular, very numerous on the area and deltidium. 
 
 The cardinal process is developed in a high degree in this species. It extends, 
 not only partially under the pseudo-deltidium of the ventral vaive, as described by Mr. 
 Davidson * in Orthotetes crenistria, but completely under it for some distance. In the 
 present specimens it is a long, rather shoe-horn shaped, testaceous projection, extending 
 either at right angles, or nearly so, from the umbonal centre of the hinge-line. In one or 
 two cases it is quite at right angles, in others it is inclined upwards. In ordinary forms 
 of Orthotetes crenistria the cardinal process is bidentate at the outer end, but in the 
 present case the terminal expanded bidentation is flanked by a lateral projection on 
 each side and always more or less perceptible, but at times much more marked than at 
 _ others, and when so considerably increasing the width of the process. 
 
 These prominent examples of Orthotetes senilis to some extent resemble the 
 variety robusta, Hall, figured by Dr. Davidson from Indian Carboniferous rocks,f only, 
 in the latter, the ventral valve appears wider across the hinge; the umbo, however, 
 projects upwards and backwards, as in the Queensland examples. 
 
 Loc. and Horizon. Pelican Creek, three-quarters of a mile above Sonoma Road- 
 crossing (&. L. Jack)—Middle or Marine Series, Bowen River Coal Field; Havilah- 
 Byerwin Road, one mile south of Rosella Creek-crossing (&. LD. Jack). The geological 
 position of this species in the Bowen River Coal Field is both interesting and peculiar. 
 According to my Colleague’s notes, the first locality above given is in his Middle or 
 Marine Series, while the second locality is in a marine band, in his Upper or Freshwater 
 Series, which is characterised by the predominance of the much-disputed genus 
 Glossopteris, and other so-called Oolitic plants. 
 
 Family—PRODUCTIDZ. 
 
 Genus—PRODUCTUS, J. Sowerby, 1814. 
 (Min. Con. i., p. 158.) 
 
 Obs. The Producti of the Eastern Australian area form a peculiar and interesting 
 group in themselves. The identity of many of the species with those of Europe is, I 
 think, vague. We certainly possess Productus cora, D’Orb., or, at any rate, a form so 
 like it that I am unable to refer to any difference, whilst other species have from time 
 to time been referred by Authors to P. longispinus, P. scabriculus, P. semireticulatus, 
 and others. I have made use of these terms even in the present Memoir, but I feel 
 that they are but names used to distinguish some cast or weathered specimen having a 
 fancied resemblance to the speciés in question. Nine-tenths of our Producti are but 
 casts, and therefore very difficult to determine, and it is not until a long and close study 
 of such from many localities has been made, that the number of species actually existing 
 can be put on a satisfactory footing. The species, however, are few,-and it is not 
 improbable that this decrease in number has to some extent been compensated for by 
 the increase, both in species and their importance, of the genus Strophalosia. 
 
 Long research leads me to the belief that great community of form existed 
 amongst the Producti of Queensland, New South Wales, and Tasmania. 
 
 Of the only two species of which sufficiently complete specimens have been found 
 to render their entire examination satisfactory, both are now known to possess an area, 
 usually well marked, always certainly present. 
 
 * Mon Brit. Carb. Brach., 1858, Pt. 4, p. 30. 
 + Quart. Journ. Geol. Soe., xviii., p. 30, t. 1, f. 16, 
 
248 
 
 Propvctus corsa, D’ Orbigny. 
 PISi2ehesiae Py 18sne. 1s Please 
 Productus cora, D’Orbigny, Pal. Voy. Amérique Mérid., 1842, iii., Pts. 3 and 4, p. 55, t. 5, ff. 8 and 9. 
 op s, Davidson, Mon. Brit. Carb. Brach., 1861, Pt. 4, p. 148, t. 36, f. 4, t. 42, f. 9. 
 AD », Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 328, t. 15, ff. 1 and 2. 
 + » Etheridge fil., Cat. Australian Foss., 1878, p. 51. 
 53 », De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 184, t. 9, f. 1. 
 
 Obs. P. cora was first detected as a Queensland fossil by Mr. Etheridge in the 
 Collection made by the late Mr. R. Daintree. His remarks were as follows :—“ Our 
 shell was evidently very thin and fragile, with a gibbous ventral valve, the surface 
 covered with straight, wavy, or flexuous longitudinal thread-like striz or ribs, and few 
 spines. The dorsal valve shows the rugose undulating folds or wrinkles at the 
 cardinal angles. We fail to see the concentric lines crossing the ribs on our examples, 
 owing to their condition ; and the places of former spines are faintly traceable.” 
 
 The surface of slabs of the chloritie rock of Gympie are often covered with 
 crushed examples of this species, and my Colleague has collected a number of similar 
 smaller Producti, both dorsal and ventral valves, which are probably identical. - 
 
 Three-quarters of a valve has also been obtained from the Rockhampton Beds, 
 showing the fine regular striation, spinose wings, and coarsely wrinkled flanks of this 
 well-marked species. A second, which may be either P. cora, or P. semireticulatus, hag 
 also been found by Mr. Smith. The flanks of this specimen are too much wrinkled for 
 the former, although the fineness of the striz would indicate P. cora as its proper refer- 
 ence. The character of the wings and the strong spines thereon do not assist in a 
 determination, as these are features common to both species. On the whole, I am 
 inclined to refer this shell, from the Training Wall Quarries, to P. cora. Exceedingly 
 well-marked casts have been collected from the rich beds of Mount Britton, by Mr. 
 A. L. Morisset, exhibiting similar features to the Rockhampton specimens. 
 
 Loc. and Horizon. New Caledonia Reef, Gympie (The late R. Daintree) ; 
 Gympie (&. L. Jack) ; Stony Creek, Stanwell (The late James Smith) ; Training Wall 
 Quarries, Fitzroy River, Rockhampton (The late James Smith)—Gympie Beds ; South side 
 of Mount Britton (A. Z. Morisset)—Middle or Marine Series, Bowen River Coal Field. 
 
 PRODUCTUS BRACHYTHERUS, G. Sowerby. 
 Pl. 12, figs. 10-18; Pl. 18, fig. 5 ?; Pl. 44, fig. 14. 
 
 Productus brachytherus, G. B. Sby. in Darwin’s Geol. Obs. Vole. Islands, 1844, p. 158. 
 
 ; 35 Morris in Strzelecki’s Phys. Descr. N. 8S. Wales, &c., 1845, p. 284, t. 14, f. 4c 
 non 4a and 4b). 
 
 i 3 De Koninck, Mon. Genre Productus, p. 241, t. 16, f. la and b (non 1c and d). 
 
 x subquadratus,, De Koninck (non Morris), loc. cit., p. 203, t. 14, f. le and d (? 1a and 6). 
 
 brachytherus, De Koninck, Mon. Productus et Chonetes, 1847, p. 102, t. 16, f. lw and b (non 
 le and d). 
 
 4 subquadratus, De Koninck (non Morris), Ibid, t. 14, f. 1c and d (? 1a and 0). 
 
 a brachytherus, Dana in Geology Wilkes’ U.S. Explor, Exped., 1849, Vol. x., p. 686, Atlas, t. 2, f. 8. 
 
 55 35 D’Orbigny, in Dumont D’Urville’s Voy. au Péle Sud, 1846, Paleeontologie, Atlas, 
 t. 6, f. 6 and 7. 
 
 AD fragilis, Dana, American Journ. Sci., 1847, iv., p. 153. 
 
 “i y Dana, loc. cit., p. 686, Atlas, t. 2, £.. 7. 
 
 39 brachytharus, De Koninck, Foss. Pal. Nouy.-Galles du Sud, 1877, Pt. 3, p. 198, t. 10, f. 4 and 4a 
 (Gis hs 0 ak ys 
 
 fragilis, De Koninck, loc, cit., p. 201, t. 10, f. 3 and 3a. 
 > brachytherus, Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 284, t. 8, f. 16, t. 9, 
 f. 17 and 18, 
 Sp. Char. Shell of medium size, subtrapezoidal to subrectangular, non-lobate, 
 more or less reflected, or geniculate, and generally gibbous. Ventral valve very gibbous 
 
249 
 
 in the visceral region, vaulted, geniculate, or reflected on itself; surface convexly 
 rounded, no sinus; sides vertical, or even sometimes slightly concave separating the 
 remainder of the valve from the more or less short, flattened, triangular ears; umbonal 
 region often depressed from above, sometimes greatly recurved, and sometimes more 
 or less incurved over the hinge-line; the latter is of median length, but a little less than 
 the width of the valve, sharp and acute; front usually much recurved and occasionally 
 laterally expanded, assisting to give the shell much of its geniculate appearance ; beak 
 small and acute ; surface, when the outer shell is preserved, shining and silky, with a few 
 growth constrictions towards the front, and indistinct undulations on the umbonal 
 region; longitudinally and indistinctly costated by delicate, elongate, parallel spine 
 bases, within the substance of the shelly matter, penetrating the latter, as small, free, 
 short, tubercle-like spines, giving a general prickly or pimply appearance to the entire 
 valve, especially towards the front. When the thin outer shell is removed, or in 
 decorticated examples, these long spine bases leave a series of fine channels on the 
 surface of the fossil. Ears with numerous tubular spines. The cardinal muscular 
 scars are but little marked ; the adductors are straight, and formed of oblique ramifi- 
 cations; surface granular. 
 
 The dorsal valve varies in the amount of its concavity, being at times shallow, 
 at others exceedingly concave, especially in the middle line; ears flattened; front 
 produced ; surface with concentric lines and spine bases. The septum is moderately 
 short; dendritic adductor impressions small; reniform impressions laterally extended, 
 and well marked; internal surface granular. 
 
 Obs. Productus brachytherus is one of the most interesting species of the genus 
 yet published, and has been much misunderstood by several of those who have written 
 about it. The species is well worth a separate and detailed study. Chance observers 
 examining the various figures hitherto published would be apt to consider them as not 
 all appertaining to one species. If full attention, however, is given to the various 
 aspects under which the shell is found, I believe it can be shown that paey one and all 
 represent a single well-marked and peculiar species. 
 
 Ali who have written on P. brachytherus lay stress on the ee eees of the hinge- 
 line as compared with the width of the front. This, with the elongated decurrent feces 
 of the spines, forming channels in the shell, are particularly iierate ite points in 
 G. B. Sowerby’s species. The channelling of the shell by the spine bases is seen in 
 many species of Productus, but it appears to be pecularly distinctive of P. brachytherus. 
 The length of the hinge-line varies according to age, in large and old individuals it 
 becomes longer, and the shell, which is very convex and geniculate, loses some of its 
 convexity and also widens out. 
 
 In describing this species the late Professor John Morris referred to it two shells 
 of very different aspect and state of preservation. One of these is a cast in sandstone, 
 showing the general form, and more particularly the channels formed by the decurrent 
 bases of the spines. The other specimen is a decorticated siliceous cast, and displays 
 the internal characters of both valves to great perfection. On the ventral valve are 
 exposed the node-like prominences of the cardinal muscles, the scars of the more 
 elongated adductor muscles, and the internal cast of the beak. The dorsal valve shows 
 the scars of the adductors, and the cast of the septum, which in this individual reaches 
 almost to the front margin of the valve, an ususual length in the genus Productus. 
 The vascular impressions are also preserved and come very far forward, like the 
 septum. 
 
 In his Work onthe “ Genus Productus,” again in that on “ Productus and Chonetes,” 
 and more recently in his “ Fossiles Paléozoiques de la Nouvelle-Galles du Sud,” Prof. De 
 
250 
 
 Koninck has expressed an opinion that the two shells in question, referred by Morris to 
 P. brachytherus, are different, and do not belong to the same species, one being possessed 
 of a short septum in the dorsal valve and less marked muscular scars, the other, on the 
 contrary, with a very long septum and strongly marked scars. In working out the 
 species it became essential for anything like correct determination that some more 
 satisfactory solution of this subject than mere opinion should be arrived at. 
 
 The specimens used by Mr. G. B. Sowerby having disappeared, as already 
 explained,* those contained in Strzelecki’s Collection in the British Museum, and 
 described by the late Prof. Morris must be accepted as the types, and to their structure 
 all future appeals must be made in determining the identity of P. brachytherus, G. Sow., 
 Morris. Now, as stated above, Prof. De Koninck regards the silicified cast + with the 
 long septum, described by Morris as P. brachytherus, to be specitically distinct from the 
 true P. brachytherus,~ a name which he considers should be retained for a form with a 
 short septum, amongst other characters. The silicified cast figured by Morris in 
 Strzelecki’s Work (PI. xiv., ff. 4a and 6) has, for one of its most distinctive characters, a 
 long septum in the dorsal valve, as previously pointed out; but the example of P, 
 brachytherus represented by the sandstone cast accorded much better with Sowerby’s 
 description of his species, than did the siliceous example. The specimen in question,{ as 
 then exposed, was that of a ventral valve backed up with matrix so that on the removal 
 of the latter the cast of the dorsal valve would be visible and the septum exposed, long 
 or short as the case might be. It was found to possess, so far as we are able to judge, 
 a short septum, so probably confirming in a remarkable manner Prof. De Koninck’s 
 surmise. The matter then stands thus: The figure given by Morris in Strzelecki’s Work 
 on “ New South Wales,” Pl. xiv., f. 4c, is the true P. brachytherus, characterised by the 
 presence of a short septum anda little developed muscular system. On the other hand 
 (Pl. xiv., ff. 4a and 4, of the same Work), the siliceous cast, with a very long septum and 
 great muscular development, is a distinct and separate species. MceCoy’s type specimens 
 of P. brachytherus, in the Woodwardian Museum, Cambridge, do not call for any 
 particular notice beyond the fact that they show the species to be in outward appearance 
 not unlike the variety pugilis, Phill., of the European species, P. semireticulatus, 
 Martin, and a peculiar streaky appearance is given.to the exterior of the shell by 
 the decurrent bases of the spines. With regard to McCoy’s P. undulatus,§ Prof. 
 De Koninck || refers it to PB. brachytherus; but a careful examination of the 
 type in the Woodwardian Museum has not convinced me of their identity. I have 
 not seen such peculiar undulating strie upon any specimen of P. brachytherus I have 
 examined. 
 
 When well preserved, and not crushed or broken, P. brachytherus is a subquadrate 
 shell, high and gibbous in the visceral region, rapidly and deeply sloping off at the 
 sides to the flat, triangular ears. Such a condition is represented by Morris’s original 
 figure, one of De Koninck’s of his so-called P. subguadratus, Morris,** and his earlier 
 figure of P. brachytherust+ and his last figure of the same species.tt The ears of this 
 species appear to have been particularly fragile, and more often than not have com- 
 
 
 
 * Proc. R. Phys. Soc. Edinb., 1880, v., p. 285. 
 + Strzelecki, Joc. cit., Pl. 14, f. 4a and b. 
 t Strzelecki, loc. cit., Pl. 14, f. 4c. 
 § Ann. and Mag. Nat. Hist., 1847, xx., p. 235. 
 Foss. Pal. Nouy.-Galles du Sud, 1877, Pt. 3, p. 198. 
 4] Strzelecki, loc. cit., t. 14, f. 4c. 
 ** Mon. Gen. Productus, t. 14, f. le. 
 +t Ibid., t. 16, f. la and 6. 
 +t Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, t. 10, f, 4a and b. 
 
251 
 
 pletely disappeared. When this is the case we find the shell assumes a subtrapezoidal 
 outline, and presents a very different appearance to that previously described. In 
 this state it is represented by another of De Koninck’s figures of P. swbquadratus,* 
 and my own from the Bowen River Coal Field+ At times a highly geniculate 
 form is assumed by P. brachytherus, with various intermediate conditions between this 
 and the former outlines. When much reflected in this way it becomes the P. fragilis, 
 Dana,{ and one of the intermediate forms is shown in another figure of my own from 
 North Queensland.§ In the Mining and Geological Museum, Sydney, is a very 
 geniculate individual from the Bowen River Coal Field, in which the depth through 
 the sheli is two inches. These are the forms usually assumed by P. brachytherus. 
 The elongated spine bases are clearly contained within the substance of the shell, and 
 when decortication takes place, the spine bases appear to be removed with the outer- 
 most shelly layers, leaving long open channels. For quite a third of the height from 
 the front margin, these spine bases are absent, and this portion bears scattered out- 
 standing spines, the intermediate portions being glossy and smooth. 
 
 Now, with regard to the reference of Productus subquadratus (Morris), De 
 Koninck, and P. fragilis, Dana, to this species. P. subqguadratus, Morris,|| was very 
 briefly described—too briefly, in fact—and in the absence of a figure would have been 
 unrecognizable, had it not been for the fact that Morris says —‘“‘ Mesial furrow broad 
 and distinct.” Herein it differs entirely from P. brachytherus. The only figures extant 
 referred to P. subguadratus are those published years ago by De Koninck,{ one of which 
 is an ordinary form of the P. brachytherus, a second is that form of this species with 
 the ears broken off, as I have above described : and the identity of the third is doubtful. 
 There can be no doubt about the second figure, the short (broken), erect, sharp hinge, 
 trapezoidal outline, short septum, and no trace of a sinus, are characters not to be mis- 
 taken. It is but just to Prof. De Koninck to say that he even doubted the accuracy of 
 his own determination, for he says—‘‘ Je ne suis pas entiérement convaincu de la réalité 
 de cette espéce, et je le n’adopte provisoirement qu’en faisant mes reserves pour l’avenir.” 
 
 Productus fragilis was the name given by Prof. J. D. Dana** to the highly 
 geniculate condition of P. brachytherus, an opinion I have previously expressed tf and 
 still adhere to. Prof. De Koninck held a contrary view, and has furnished an elaborate 
 description of what he believed to be P. fragilis, Dana, in his recent Work.tt 
 
 So little reliance can be placed on some of the late Prof. De Koninck’s descrip- 
 tions, this amongst the number, that it is extremely difficult to grasp the requisite 
 characters for the detection of the species then running in the mind of the Author. He 
 states that the dorsal valve of P. fragilis is “legérement concave’’; but some few lines 
 further on, on the next page, when comparing the species with P. brachytherus, he 
 nullifies this statement by saying, “la convexité de sa valve dorsale.’’ It is quite 
 possible, as he observes further on, that the shell he is describing as P. fragilis may be 
 identical with the unnamed siliceous casts in Strzelecki’s work, previously referred to 
 (t. 14, f. 4a-b). Of the true P. fragilis, Dana, however, I am in no doubt. I fail to 
 see how it can be anything more than a variety of the species now under description. 
 
 * Mon. Gen. Productus, t. 14, f. 1d. 
 
 + Proc. R. Phys. Soc. Edinb., 1880, v., t. 8, f. 16. 
 
 + Geology Wilkes’ U. 8. Explor. Exped., 1849, Vol. x., Atlas, t. 2, f, 17. 
 
 § Loc. cit., t. 9, £. 17 and 18. 
 
 || Strzelecki’s Phys. Descrip. N. 5. Wales, &c., 1845, p. 284. 
 
 {| Mon. Gen. Productus, p. 203, t. 14, f. la-d. 
 
 ** Geology Wilkes’ U. 8. Explor. Exped., 1849, Vol. x., p. 686, Atlas, t. 2, f. 7. 
 +t Proc. R. Phys. Soc. Edinb., 1880, v., p. 287. 
 
 tt Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 201. 
 
252 
 
 As compared with Productus scabriculus, the present one is much more geniculate, 
 but they frequently otherwise resemble one another in shape. Our species does not 
 possess a divided septum in the dorsal valve ; but, on the other hand, an area is present, 
 the surface of the dorsal valve is far more concave, and the spine bases on the surface 
 of the ventral valve quite lack the regular and close arrangement of those of P. 
 scabriculus. 
 
 As a rule, when examined in the state of casts, the muscular scars of P. 
 brachytherus do not appear to be highly developed, and, as compared with similar 
 features in P. subquadratus, there is a marked difference. But in examples of the former 
 from the Darr River,* in which the whole of the shelly matter is practically retained, 
 this difference is not of so marked a character, and it is further evident both that the 
 shell attained a very considerable thickness, and that a distinct area was present (Pl. 
 44, fig. 14). This varies much in breadth, sometimes becoming quite linear, and at 
 other times broad and appreciable. 
 
 Loc. and Horizon. Stonehumpy Creek, and Pelican Creek, near No. 1 Bore 
 (R. LZ. Jack)—Middle or Marine Series, Bowen River Coal Field; Havilah-Byerwin 
 Road, one mile south of Rosella Creek-crossing (2. ZL. Jack)—Marine band in the 
 Upper or Freshwater Series, Bowen River Coal Field, associated with Derbyia senilis ; 
 Fenestella Hill, Encrinite Creek, and Stony Creek, Stanwell, near Rockhampton (Zhe 
 late James Smith) ; Limestone, close to Yarrol Station, Burnett (W. H. Rands) ; Spring 
 Creek, Cania, Burnett (W. H. Rands)—Gympie Beds; Darr Rivert (Prof. A. 
 Liversidge) ; Richards’ Homestead, three miles south-west of Mount Britton Town- 
 ship (A. LZ. Morisset)—Middle or Marine Series, Bowen River Coal Field. 
 
 Propuctus suBQuaDRATUS, Morris, Pl. 38, figs. 7-10; Pl. 40, fig. 5. 
 
 Productus subquadratus, Morris in Strzelecki’s Phys. Desc. N. S. Wales, &c., 1845, p. 284. 
 
 De Koninck, Mon. Gen. Productus, p. 203, t. 14, f. la and 0. 
 
 De Koninck, Mon. Productus et Chonetes, 1847, p. 100, t. 14, f. la and 6. 
 xD -~ Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 283. 
 
 Sp. Char. Shell large, quadrate-triangular, inflated, gibbous, and very geniculate, 
 being produced much towards the front; when viewed laterally the sides are wall-like, 
 but when seen from the dorsal side the shell has a more expanded appearance. Ventral 
 valve very convex and much curved, inflated about the middle of the shell; a well- 
 marked sinus usually extends from the umbonal region continuously to the front margin, 
 shallowing towards the latter, and giving to the valve a more or less bilobed appear- 
 ance; sides vertical, and flattened ; umbo large, thick, incurved, but not overhanging 
 the hinge-line, or produced beyond it; area shor§ and triangular, transversely striate ; 
 pseudo-deltidial aperture triangular and very marked, the area on each side below it 
 sometimes thickened into a blunt prominence (hardly teeth) ; adductor scars deeply 
 impressed, forming prominent oblong or oval eminences in casts, vertically ridged and 
 grooved, cardinal scars narrow, elongate and deep, the median dividing groove very 
 linear; umbonal cavity much pitted and grooved. Dorsal valve flattened above, 
 becoming concave and geniculate towards the front, when the valve often becomes bent 
 almost in the form of a right angle; hinge-line rather shorter than the width of the 
 valve, with the alar angles rounded; area longer and narrower than in the ventral 
 valve; septum entire, strong, sharp, extending to within a short distance of the front 
 edge, and distally projecting as a thick and strong cardinal process far into the 
 umbonal cavity; alar ridges inconspicuous ; adductor impressions in deep depressions, 
 
 9) 9 
 
 99 9 
 
 
 
 
 
 
 
 * There must be some mistake as to the lccality of this example, as the Darr River is wholly in the 
 Rolling Downs Beds. Perhaps the ‘‘ Don,” near Rockhampton, is the river referred to. (R.L.J.) 
 + Locality doubtful. (&.Z.7.) 
 
2538 
 
 circumscribed by the strong prominent encircling ridges, higher than wide, and vertically 
 dendritic ; reniform impressions oval, large, and faintly marked, the limbs quite 
 horizontal. Surface of both valves with alternate rows of tear-like tubercles, arranged 
 roughly in quincunx, giving support to short free spines, the whole interrupted by a few 
 concentric undulations. 
 
 Obs. The above characters are taken both from specimens with the outer 
 shell more or less preserved, and excellent internal casts. It occurs in some profusion 
 near Mount Britton Township, in the latter condition (Pl. 38, figs. 7-10) exhibiting 
 many of the characters in great beauty. 
 
 This is probably the largest of the Australian Producti, even exceeding P. cora 
 in size, which it resembles somewhat in outline. It is remarkable for its massive and 
 geniculate form, wide open sinus, and straight wall-like sides, characters to some extent 
 commented on by Morris. 
 
 The umbo of the ventral valve is fairly large for the size of the shell, doubtless 
 to provide room for the large proximal end of the cardinal process, and although 
 incurved, is not produced to overhang the hinge-line. Without doubt there isan area 
 in both valves, which is always short and triangular in the ventral, but seems to be 
 longer in the dorsal. That of the former is excellently shown in its most exaggerated 
 form in a specimen from Yatton, in which nearly the whole of the shelly matter is pre- 
 served. The area of both valves, when united, is seen in several specimens from Mount 
 Britton, but more particularly on the impression of a large valve, three by three and 
 a-half inches in size, from Lake’s Creek. Here the dorsal margin is thickened, forming 
 an area nearly one-eighth of an inch wide, and delicately transversely striate. This, 
 and the triangular pseudo-deltidial aperture, are characters which do sometimes occur 
 in Productus proper, as, for instance, in the specimen of P. semireticulatus figured * by 
 the late Dr. T. Davidson, from the English Carboniferous Limestone. He remarked on 
 this—“ Possesses sometimes, although rarely, a well-defined area and fissure covered by a 
 pseudo-deltidium.” The presence of the blunt protuberances, one on each side of the 
 fissure, have already been referred to in the Yatton shell, and it might be argued that 
 from the presence of these we are dealing with a Strophalosia ; but the reniform impres- 
 sions are clearly those of Productus, so that any reference to the former must be 
 abandoned. Could we be certain that these callosities represent hinge teeth received 
 into sockets on the opposite, or dorsal valve, the genus Productella, Hall,f would put in 
 a much stronger claim. In this genus there are a “ narrow area on each valve, a foramen 
 or callosity on the ventral area, small teeth, and more or less distinct teeth sockets.” 
 But Iam by no means sure that these thickenings are any more than so, and do not 
 actually represent hinge teeth in the sense of those seen in Strophalosia and Productella. 
 
 The adductor muscular scars of the ventral valve are placed low down, and are 
 dendritic (Pl. 40, fig. 5). In Productus, as a rule, these scars are elongately reniform, 
 but in a few species, such as P. humerosus{ and P. lineatus, Waagen, they resemble 
 the examples now before us. Taking, therefore, the general structure of P. subguadratus, 
 it will be found to depart considerably from the restricted description of Productus, and 
 marks a transition towards those ponderous and abnormal shells called Productus 
 comoides and P. llangollensis, by Mr. Davidson.§ In Dr. Waagen’s later classification 
 of the Productide, these are made the types of a new genus Daviesella,|| and rightly so. 
 
 * Mon. Brit. Carb. Brach., Pt. 4, t. 43, f. 5. 
 
 1 Pal. IN. York, 1867, 1v., p. 153: 
 
 { Mon. Brit. Carb. Brach., 1861, Pt. 4, p. 147, t. 36, f. 1 and 10. 
 
 § Loc. cit., 1862, Pt. 5, t. 55, f. 8 and 9. 
 
 || Pal, Indica (Salt Range Fossils), 1884, Ser, xiii., Vol. i., No. 4, fas. 4, p. 613, 
 
254 
 
 They, however, differ from Productus, restricted, in the presence of supplementary 
 adductor sears, which are certainly not visible in any of the Australian specimens 
 examined by me. Under these circumstances, P. subquadratus must for the present 
 remain in the older genus, although it would probably simplify the classification of such 
 intermediate forms if another genus were established for them, differing from Productus 
 as above indicated, and agreeing with Daviesiella in all but the character named. The 
 casts of both the dorsal and ventral valves are much pitted towards the front margin, 
 and the general surface of the former is covered with pockmark-like depressions. 
 
 P. subquadratus is distinguished from P. brachytherus by its much larger size, 
 sinus of the ventral valve, length of the septum, much larger area, and lastly the 
 dendritic adductor scars of the ventral valve. 
 
 There are some points in common between the present species and Productus 
 scabriculus, Martin, such as the bilobate form of the ventral valve, the sinus, and 
 generally speaking, aC ornamenting spines. Unlike the British species, however, our 
 form is remarkably geniculate, is really more deltoid, and not so transverse. Further- 
 more, the septum is here entire, of great length and development, and the reniform 
 impressions much more lateral in position, and placed lower down. A single specimen 
 of P. scabriculus has been recorded by De Koninck from New South Wales, and the 
 description leads me to infer that the Author had before him some condition of the 
 present species. 
 
 Near to P. subquadratus is Productus Purdoni, an Indian species described by the 
 late Dr. Davidson,* both in the form of the shell and general surface characters ; but 
 the Indian species is not geniculate, and has a pronounced fold in the dorsal valve. 
 Neither of the numerous examples of the former shell examined by me have shown this, 
 nor the fine reticulation of the surface described in P. Purdoni by Dr. Waagen.t 
 
 Before concluding, a few words must be said about the siliceous cast figured by 
 Morris as Productus brachytherus,{ and which, although now known not to be that 
 species, is at the same time in want of determination. It possesses many points in 
 common with P. subguadratus, and in the figure there is a very suspicious indication of 
 an area. If the ventral adductor scars could only be shown to be dendritic, the 
 resemblance would be complete. I think it not impossible that we are dealing here 
 with a small and short form of the present species. 
 
 Loe. and Horizon. Richards’ Homestead, three miles south-west of Mount 
 Britton Township (4. LZ. Morisset) ; Pelican Creek, two and a-half miles above Sonoma 
 Road-crossing (2. L. Jack)—Middle or Marine Series of the Bowen River Coal Field 
 Lake’s Creek, near Rockhampton (Zhe late James Smith); Yatton Gold Field (2. L. 
 Jack)—Gympie Beds. 
 
 Propuctus unpatus, Defrance, Pl. 12, fig. 16. 
 
 Productus undatus, Defrance, Dict. Sci. Nat., 1826, xliii., p. 354. 
 +3 2 Davidson, Mon. Brit. Carb. Brach., 1861, Pt. 4, p. 161, t. 34, f. 7-13. 
 AA m De Roninol Foss. Pal. Nouy.-Galles du Sud, 1877, Pt. 3, p. L90, t. 11, f. 4. 
 x, 6 Etheridge fil., Cat. Australian Foss., 1878, p. 53. 
 
 Obs. This species is known only by a single specimen, exhibiting the regular 
 concentric undulations characteristic of it. The latter are much more uniform and 
 continuous than those on the figure of the example from New South Wales given by 
 
 
 
 * Quart. Journ. Geol. Soc., 1861, xviii., p. 31, t. 2, f. 5a and b. 
 + Pal. Indica (Salt Range Fossils , 1884, Ser. xiii., Vol. i, Pt. 4, fase. 4, p. 705, t. 73, £. 1-3. 
 + Strzelecki’s Phys. Descrip. N. S. Wales, &c., t. 14, f. 4a and 0. 
 
255 
 
 Prof. De Koninck. The terrace-like undulations are much too pronounced and coarse 
 for the wavy lines ornamenting the surface of P. widulatus, McCoy,* otherwise there 
 is some resemblance between the two forms. 
 
 Loe. and Horizon. Stony Creek, Stanwell, near Rockhampton (The late James 
 
 Smith)—Gympie Beds. 
 
 PRODUCTUS SEMIRETICULATUS, Jartin, sp. ? 
 
 Conch. (Anomites) semireticulatus, Martin, Pet. Derb., 1809, t. 32, f. 1 and 2, t. 33, f. 4. 
 Productus semireticulatus, Davidson, Mon. Brit. Carb. Brach., 1861, Pt. 4, p. 149, t. 43, f. 1-11, t. 44, f. 1-4, 
 £ - De Koninck, Foss. Pal. Nouv-Galles du Sud, 1877, Pt. 3, p. 188, t. 9, f. 2. 
 
 Obs. Small, partially decorticated casts, with the long hinge-line, alar spines, and 
 chequered surface of this species have been collected by Mr. James Smith and Mr. 
 Rands. The length of the hinge-line, amongst other characters, distinguishes it from 
 P. brachytherus. 
 
 Loc. and Horizon. Stony Creek, Stanwell, near Rockhampton (The late James 
 Smith) ; Spring Creek, Cania, Burnett (W. H. Rands)—Gympie Beds. 
 
 Propwuctus Loneispinus, J. Sowerby, ? Pl. 13, fig. 2. 
 Productus longispinus, J. Sby., Min. Con., 1814, i., p. 154, t. 68, f. 1. 
 
 7 Ag Davidson, Mon. Brit. Carb. Brach., 1861, Pt. 4, p. 154, t. 35, f. 5-19 (for general 
 synonymy). 
 vi 7 Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 333, t. 18, f. 9. 
 
 Obs. This common and widely spread shell is the most variable of the Producti, 
 and seldom attains a larger size than our specimen, which is a east of the interior of the 
 dorsal valve. It is known in the Carboniferous Limestone of the Punjaub, in India, 
 Carro Creek in Tasmania, Bolivia, Russia, and Belgium, and everywhere in Britain; we 
 now, for the first time, record it from Queensland. (Ltheridge.) 
 
 Loe. and Horizon. Don River (The late R. Daintree)—Gympie Beds. 
 
 Propvuctws, sp. ind. (a), Pl. 18, fig. 6. 
 
 Obs. A peculiar form which must, for the present, from the want of sufficient 
 material, remain undetermined, has been obtained in the Burnett District. Specimens 
 consist of decorticated casts, with well-separated, distinct, fine, string-like radiating 
 coste. Such are found in some varieties of Productus giganteus, Martin. They are 
 not reticulate like P. semireticulatus, and the ribs are too coarse for a variety of 
 P. cora, although characters ix common with each of these species are present. The 
 sharp and incurved condition of the beak of the ventral valve indicates a transition 
 towards Productus striatus, some forms of which occasionally possess coarse strie. 
 
 Loe. and Horizon. Near Yarrol Station, Burnett District (W. H. Rands)— 
 Gympie Beds. . 
 
 Propvctrvs, sp. ind. (6.), Pl. 12, fig. 15. 
 [Compare P. fimbriatus (Sby.), Davidson, Mon. Brit. Carb. Brach., 18 1, Pt. 4, t. 33, f, 13.] 
 
 Obs. A very remarkable and interesting fragment presented itself on a slab, 
 with other fossils, from the prolific beds of Stanwell, consisting of the outer shell of a 
 Productus, seen from the inside. The spine bases are serially arranged in concentric 
 rows, after the manner of those of Productus fimbriatus, Sby., whilst around the edge 
 of the shell they are visible in section diverging from the surface of the valve. There is 
 not the irregularity of disposition seen in the spines of P. aculeatus, but, on the con- 
 trary, the bases are on rather raised concentric rims, as in the species first mentioned. 
 
 * Ann. and Mag. Nat. Hist., 1847, xx., p. 236, t. 13, f. 2. 
 
256 
 
 The umbonal region and hinge-line are, unfortunately, not preserved, and in consequence 
 a direct reference to Productus may have elements of doubt, but, at the same time, I 
 cannot satisfactorily compare it to any other Brachiopod. The spines are too coarse 
 and much too far apart for either an Athyris, such as A. Roysii, or a Reticularia, like 
 R. lineata. Wad it not been for the regular concentric method of arrangement of the 
 spine bases, P. spinulosus, J. Sby., might have put in a claim for comparison. 
 
 Loc. and Horizon. Stony Creek, Stanwell, near Rockhampton (Lhe late James 
 Smith)—Gympie Beds. 
 
 Propvuctws sp. ind. (¢.), Pl. 13, Fig. 4. 
 [Compare Productus prwlongus (Sby.), Davidson, Mon. Brit. Dey. Brach., 1865, Pt. 2, p. 602, t. 19, f. 22-25. ] 
 
 Obs. A very remarkable fragment is represented in the above figure. It is the 
 external impression of the ventral valve of a Productus, regularly and delicately striate, 
 with a slight median ridge, representing the cast of the mesial sinus, on which are five 
 pits ina line. These are the impressions of spines, and both the position of them and 
 the general appearance of the fossil, strongly recall to mind the structure of Productus 
 prelongus, Sby. It is, however, probable that the shell possessed a more regular shape 
 than that species. A similar distribution of spines is met with in Productus mesolobus, 
 Phill., to some extent, accompanied by other characters which are not present in our 
 fossil. 
 
 Lec. and Horizon. Stony Creek, Stanwell, near Rockhampton (Lhe late James 
 Smith)—Gympie Beds. 
 
 Propvctvs, sp. ind. (d.), Pl. 40, fig. 4. 
 
 Obs. A small and peculiar, partially decorticated specimen of the P. costatus 
 group. It is a ventral valve with along straight hinge, depressed broad visceral regions, 
 irregularly and concentrically wrinkled, whilst the central front, and that portion of the 
 surface only, bears distinct, fine, and well separated vertical ribs, the sides being free. 
 Some of the ribs bifurcate, whilst others seem to have been spined. The concentric 
 wrinkles are strongly marked on the alar expansions. 
 
 Only one example of this peculiar little shell has come under my notice, 
 otherwise I believe the characters are sufficiently peculiar to warrant a name being 
 given to it. The form and nature of the coste indicate P. costatus as the group to 
 which it is referable, but in this species the whole of the front bears ribs, except a very 
 limited portion of the ears, but in our specimen the limitation is a very marked one. 
 In a like manner it differs from the allied Indian species Productus indicus, Waagen, 
 P. vishnu, Waagen, &e. 
 
 Loc. and Horizon. Rockhampton District * (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 Propucrovs, sp. znd. (e.), Pl. 37, fig. 18. 
 [Compare P. Humboldti, D’Orbigny, in Waagen, Pal. Indica (Salt Lake Fossils), 1884, Ser. xiii., Vol. i., 
 Pt. 4, fase. 4, p. 695, t. 76, f. 1-3.] 
 
 Obs. This peculiar and well-spined form has caused me much trouble, and I am 
 not even now prepared to say to which of the known species it should be referred. It 
 is a decorticated cast of a rather transverse ventral valve, with a moderately long hinge- 
 line, a wide open sinus, a well ineurved beak, and vertically elongated, somewhat tear- 
 shaped spine bases arranged roughly in quincunx, those of one row alternating with 
 
 
 
 * See note, p. 199. 
 
257 
 
 those of another. The alar expansions are covered with minute short prickles. At one 
 time I took this to be either the young state of Productus subquadratus, or a peculiar 
 condition of P. brachythwrus, and I am not prepared to deny that it may not be one or 
 the other even now. However, in many points the specimen has even a closer 
 resemblance to Dr. Waagen’s figures of three Indian species—P. Hwmboldti, D’Orb., 
 P. Abichi, Waagen,* and P. serialis, Waagen.t The shape is identical, the clustering 
 of the prickle-like spines on the wings the same, the broad undefined sinus similar, and 
 above all the long tear-like quincuncially arranged body spines in every way like those on 
 our specimen. ‘The only difference I can detect—but this may result from the fact that 
 the latter is not perfect towards the front margin —is the absence of the closely clustered 
 and smaller spines all round the front of the shell, and similar to those on the alar 
 expansions. These forma very marked feature of the Indian shells. Whatever may prove 
 to be the identity of the present form, there remains the fact that we have in the Queens- 
 land beds one in many respects closely similar to forms found in India, more particularly 
 that called by Waagen Productus Abichi. I say “called” because it seems to me that 
 Dr. Waagen has figured under three separate names what might, with great advantage to 
 science, have been confined to one. All three species, P. Humboldti, P. Abichi, and P. 
 sertalis, so closely resemble one another, that I think only the Author himself could 
 Separate them. Of the two first, Dr. Waagen candidly states it to be “solely a matter 
 of taste whether the difference be admitted or not as sufficient for the distinction of two 
 separate species.” The difference consists simply of a “coarser tuberculation, and 
 by the more elongated form of the tubercles.” P. serialis is said to differ from 
 P. dAbichi by a well-developed concentric folding in a more or less close relation 
 to the spines distributed on the surface of the ventral valve. I regard all three 
 species as one, therefore, which may be known under the name of Productus Humboldti, 
 as originally determined by Dr. Davidson.t 
 
 There is the bare possibility that this may be a Strophalosia, The spines have 
 greatly the appearance of those of this genus, but I have not seen any evidence of the 
 teeth or sockets of the hinge-line. In my Paper on the Permo-Carboniferous Fossils 
 from North-West Australia, I omitted to mention that the shell there named Productus 
 brachytherus, and which is certainly the same as that now figured, possessed a depressed 
 vertical groove on the beak, after the manner of some Strophalosie. 
 
 Loc. and Horizon. Richards’ Homestead, three miles south-west of Mount 
 Britton Township (R. Hull)—Middle or Marine Series of the Bowen River Coal 
 Field. 
 
 Propuctts, sp. ind. (f.), Pl. 44, fig. 18. 
 
 Obs. A small form, which cannot be passed over, from the fact that the shell is 
 preserved. It recalls to mind, in a very curious manner, the young condition of one of 
 the varieties of the common Productus giganteus of the European Carboniferous rocks. 
 The body of the shell is large and gibbous, as compared with the small and sharp ears, 
 and transversely oblong in shape. The umbone is obtuse and much incurved, and the 
 surface covered with fine, separate, thread-like direct ribs, and the small ears delicately 
 wrinkled. In fact I never saw a closer resemblance in miniature to the above species 
 than in this little shell. 
 
 Loc. and Horizon. Yatton Gold Field (R. L. Jack)—Gympie Beds. 
 
 
 
 
 
 * Pal. Indica (Salt Range Fossils), 1884, Ser. xiii., Vol. i, Pt. 4, fas. 4, t. 74, f. 1-7. 
 + Ibid., t. 74, £. 8a-d. 
 + Quart. Journ. Geol. Soc., 1862, xviii., p. 32, t. 2, f. 6. 
 
258 
 
 Genus—STROPHALOSTIA, King, 1844. 
 Ann. and Mag. Nat. Hist., 1844, xiv., p. 313; Mon. Permian Foss. England, 1850, p. 93.) 
 
 STROPHALOSIA CLARKEI, Etheridge, sp. 
 Pl. 18, figs. 12-17,; Pl. 14, fig) 19: 
 
 Productus Clarkei, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 334, t. 17, f. 2 and 2a-b, t. 18, f. 4-4a. 
 ” i De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 208, t. 10, f. 5, t. 11, f. 2. 
 ” Etheridge fil., Cat. Australian Foss., 1878, p. 51. 
 
 Strophalosia Clarkei, Etheridge fil., Proc. R. Phys. Soe. Edinb., 1880, v., p .289, t. 9, f. 18a-21, t. 10, 
 f, 22-98, t. 11, f. 29-31, t. 12, f. 32 and 33, 
 55 Woodsit, Davidson ane 
 
 Sp. Char. Shell rotundate-quadrate, ventral valve strongly gibbous, or 
 inflated ; prominent and convex about the visceral region, sloping gradually off to the 
 front, bat non-geniculate and unproduced. Hinge-line straight, but not equal to the 
 width of the shell. Ears flattened, small when compared with the general proportions 
 of the valve. Beak large, short, ana blunt, but not overhanging the hinge-line; imme- 
 diately under it are two lar rere, obliquely placed teeth, which “fit into the Sbokets of the 
 dorsal valve. In the umbonal region of the shell, proceeding from the beak towards 
 the front, is a fine ridge or septum (a groove in casts) with, on each side of it, the 
 dendritic adductor muscular impressions, each bounded on its outer margin by a well 
 defined groove (ridges in the cast). Immediately in front of these adductor impressions 
 is a large blunt prominence (which in the cast becomes a hole or fossa of varying depth, and. 
 of a very marked character), with the outer edge much less precipitous than the inner. 
 On each side this prominence are the depressed scars of the cardinal muscles, much deeper 
 and more impressed on their inner or umbonal margins, and gradually dying out laterally 
 towards the sides of the valve; they are vertically grooved and ridged. (In the cast 
 these impressions become ridged prominences, projecting or searp-like along their upper 
 edges, and they impinge somewhat on each side over the deep fossa just described.) 
 The interior surface of the valve is pitted and ridged, producing, in the cast, granules 
 and grooves; the former are continued over the surface of the blunt prominence (fossa 
 in the cast) ; the ridges seen on the interior represent the decurrent bases of spines. 
 The exterior surface is comparatively plain, with fine, vertical, wavy lines, projecting 
 from which are occasional slender spines. 
 
 The dorsal valve is square, oval, flat, and very thick, bevelled outwardly from the 
 interior on the front margin. The latter is apparently continuous, and not indented in 
 any way. Hinge-line with rounded alar angles; area well marked, but not broad. 
 Cardinal boss thick, strong, and prominent, projecting from the hinge-line at an angle of 
 119°, with the exterior plane of the valve centrally divided by a groove, which is 
 flanked on each side by a kind of shoulder. Sockets for the reception of the teeth of the 
 ventral valve, deep, broad, and so far surrounding the boss as to produce an appearance 
 of isolation in the latter from the remainder of the valve. The cardinal boss is 
 supported on each side by indistinct, oblique, alar ridges. Septum strong and ridge- 
 like, extending for more than two-thirds the distance hetween the cardinal boss and the 
 front margin, sometimes terminating in a small button. Immediately under the boss 
 is a deep Sbsieera divided in the Fiddle line by the septum, and in which are situated 
 the dendritic adductor muscular impressions. This depression is separated by a 
 transverse ridge running across the valve from a second heart-shaped depression 
 similarly divided by ie septum. The reniform impressions are narrow, semilunar, 
 much incurved, and abrupt at their front termination, and bounded outwardly by a deep 
 groove or linear depression following their course. The internal bevelled edge is 
 marked with very fine granules of pustules and small veinings, being the indications of 
 
 ’ P 
 EE 
 
259 
 
 the vascular system. The shell has a silky appearance, and when weathered or decorti- 
 cated, the shell-substance is marked by a series of fine, wavy, vertical lines. The valve 
 is externally ornamented with a number of close, concentric, scaly lamine and a few 
 scattered spines similar to the ventral. A series of spines are also placed along the 
 hinge of the ventral valve, erect, and graduating outwards from the umbo. 
 
 Obs. The history of Strophalosia ieee is a brief one. It was originally 
 described by Mr. Etheridge as a Productus, from indifferent material in the Daintree 
 Collection, and the external characters defined. Subsequently Prof. De Koninck placed 
 under this name a shell in the W. B. Clarke Collection, and described it in his New 
 South Wales Work. In my “Catalogue” I follow both these Authors in placing the 
 species under the genus Productus, but had not then enjoyed an opportunity of examin- 
 ing specimens. 
 
 This interesting species, at the time my former description was written,* was 
 known under two conditions only—internal casts of the ventral valve, and dorsal valves 
 retaining more or less of their shelly matter. More recently I have enjoyed the 
 opportunity of examining no less than thirty-three excellently preserved specimens in 
 the Mining and Geological Museum, Sydney, from New South Wales localities, several 
 of which have the valves united. Nothing is brought more prominently forward by 
 these specimens than the flatness and non-spinous condition of the dorsal valve, and 
 herein, it appears to me, we have, in conjunction with the comparative absence of spines 
 from the ventral valve, excellent specific characters for the separation of S. Clarkei from 
 allied forms. 
 
 If we examine casts of the ventral valve, and compare them with the fine interior 
 of S. Goldfussi, Miinster, figured by the late Dr. Davidson,t it will be observed that in 
 fig. 9, representing a cast in a similar state of preservation to our specimens, there is, 
 as in the latter, the corresponding blunt and gradually attenuated but prominent beak 
 (figs. 29 and 30,7,7) ,¢ and deep pits left by the teeth of the ventral valve (fig. 30,¢). Again, 
 compare, in fig. 10 of the “ Permian Monograph,’ the concave or grooved back of the 
 umbo with that of the Queensland cast (figs. 27-30,0). Thirdly, the position of the 
 adductor scars in the same Permian figure is quite comparable with that of the Australian 
 specimens (figs. 26-30,c,c,c,c). In Mr. Davidson’s figure, the deep pit or fossa in front of 
 these impressions is not so marked as in our fig. 29; but this is itself a variable point 
 in the Australian shells. With regard to the cardinal muscular scars, we observe a 
 perfectly similar arrangement—the position identically the same, similar ridging and 
 grooving, the only apparent difference being that in the Permian 8. Goldfussi the 
 abrupt or scarp-like side appears to be towards the front, whereas in 8. Olarkei it is 
 towards the umbo or the hinge-line (figs. 27 and 29,¢,¢,e,e). It must, however, not be 
 forgotten that all these characters are open to much variation in development, but not 
 in feature, being very pronounced in some individuals, and feeble in others. 
 
 Itis strange that, out of the large series obtained by my Colleague from the Bowen 
 River Coal Field, so fow specimens should retain traces of the septum, reniform impres- 
 sions, and other anatomical details. The usual condition under which the dorsal valves 
 of 8. Clarkei are presented to us is shown by figs. 18a, 19, and 20, a flat, bevel-edged, 
 more or less oval, silky shell, and, although viewed from the interior in each case, no 
 trace of the marked characters of figs. 21 and 23 are visible, but on the contrary 
 there is, in the place of the strong cardinal boss and septum, an oval gap in the shell 
 
 * Proc. R. Phys. Soc. Edinb., 1880, v., p. 289. 
 
 + Mon. Brit. Permian Brach., t. 8, figs. 9-10. 
 
 + These numbers and letters refer to the figures given in my former description of S. Clarkei (Proe, 
 R. Phys, Soc. Edinb., 1880, v.). (R. #., Junr.) 
 
260 
 
 substance. This discrepancy between such examples as figs. 18a and 21 can be accounted 
 for simply by decortication, because, on several specimens, traces of much shelly matter 
 remain, which, if wholly preserved, would bring the shell up to the thickness required to 
 make it correspond with fig. 21 or fig. 23. 
 
 The dorsal valve is invariably flat, or, at any rate, what little concavity there is, is 
 simply a median depression. The surface is composed of scaly concentric lamine, with 
 wavy cross-lines and an occasional small spine. In specimens with the valves in apposi- 
 tion the relatively narrow and long area, as compared with that of the succeeding species, 
 becomes very apparent. 
 
 Tn the Memoir on the Bowen River Coal Field fossils, three species of Australian 
 Strophalosie were described, the present one, the succeeding species, 8S. Gerardi, and 8. 
 Jukesii. At that time much doubt existed as to the limitation of these species, but now, 
 I believe, I am in a position to satisfactorily place all three on a firmer footing. The 
 distinguishing features of §. Clarkei have already been pointed out; its relation to 8. 
 Gerardi will be shown under that species, but a few remarks on S. Jukesii may be made 
 here. 
 
 The chief point relied on formerly for the separation of §. Clarkei from 8. 
 Jukesii, was the deltoid or sub-quadrate form of the latter, as compared with the broad 
 oval outline of the former. It appears to me now that the internal characters of the 
 dorsal valve afford a far better ground for separation. In S. Clarkei the septum 
 extends almost the whole width of the dorsal valve, but in S. Jwkesiz it hardly does 
 more than reach the middle of the valve. The deeply excavated cordate depressions 
 on each side the septum of the former is absent in the latter. In the first-named 
 species the renal impressions form together a broad oval curve, and terminate forwards 
 in a line with the front end of the septum; in the second species, on the other hand, the 
 renal scars are much more aurate, comparatively broader, but not so oval, and project 
 towards the front far beyond the termination of the septum. These characters, when 
 viewed together, present a very different appearance in the two species. 
 
 The original specimens on which I described S. Jukesii were said to have come 
 both from New South Wales and Tasmania, but I believe this will prove a far more 
 representative species of the latter than the former country. 
 
 Loc. and Horizon. Pelican Creek, Bowen River, five miles north of Sonoma 
 Station ; the same, opposite Palmer’s Old Station; the same, three-quarters of a mile 
 above Sonoma Road-crossing ; Parrot Creek, Bowen River, four and a-half miles, eight 
 miles, and nine miles up; Cockatoo Creek, Bowen River, half-a-mile above junction with 
 Parrot Creek ; Bowen River, two miles above Beasley’s Old Public House (R. L. Jack) ; 
 Springsure (The late James Smith) —Middle or Marine Series of the Bowen River Coal 
 Field. 
 
 STROPHALOSIA GERaRDI, King. 
 Pl. 13, fig. 18; Pl. 14, fig. 18; Pl. 40, figs. 7 and 8. 
 
 Strophalosia Gerardi, King, Ann, and Mag. Nat. Hist., 1846, xviii., p. 98. 
 
 De Koninck, Mon. Productus et Chonetes, 1847, p. 137. 
 
 King, Mon. Permian Foss. England, 1850, p. 96, t. 19, f. 6 and 7. 
 
 Davidson, Mon. Brit. Foss. Brach., Introdaction, 1857, t. 8, f. 211. 
 
 Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 294, t. 12, f. 34-37, t. 13, £38. 
 Etheridge fil., Journ. R. Soc. N. S. Wales for 1883 [1884], xvii., p. 87. 
 
 39 
 Sp. Char. Shell of medium size, ovato-rotund, at times becoming almost deltoid, 
 strongly concavo-convex. Ventral valve convex, most so about the umbonal and visceral 
 regions; umbo prominent, rounded, and overhanging the area to some extent; area 
 short, high, and triangular ; dorsal valve varying from coneave to semi-concave, following 
 closely the contour of the ventral, assuming a more or less deltoid form, usually much 
 
 99 
 
 ee OOO eee 
 
261 
 
 longer than wide; hinge-line variable in length but never as wide as the shell; area 
 well marked, elongately triangular; deltidium conspicuous, convex; septum short; 
 renal impressions broadly oval ; internal surface highly granular. Surface of the ventral 
 valve concentrically laminated, and giving rise to numerous adpressed tapering spines, 
 which, when worn off, leave the valve covered by a series of short, blunt, somewhat 
 projecting tubercles ; surface of the dorsal valve similarly ornamented, but the concen- 
 tric lamin appear to be smaller and closer together ; near the front edge of the valve the 
 lamellz become very close and numerous, and assume a strongly imbricated appearance. 
 The greatest concavity of the dorsal valve is just below or in front of the hinge-line, where 
 it appears to become much pressed in. The shell at times assumes a slightly irregular 
 aspect, with an inclination or oblique tendency towards one side or the other; the front 
 margin is rounded and continuous, and shows no indication of an indentation or sinuosity. 
 
 Obs. The identity of this Indian species with shells from the Bowen River Coal 
 Field was based on certain individuals from the latter, possessing, amongst other 
 characters, very concave dorsal valves. This separation was made, to some extent, on 
 the advice of the late Dr. Davidson, but it was hinted that perhaps the one might prove 
 to be a variety of the other.* The following remarks on this subject were made :— 
 “Notwithstanding the flat valve of typical specimens of 8. Clarke, it is just possible: 
 that it and the shells now referred to 8S. Gerardi, with the concave dorsal valves, may 
 after all be one and the same. . . . . On the one hand we have aseries of dorsal 
 valves, all flat, and no ventral valve attached (=. Clarkez) ; on the other hand, a number 
 of bivalve examples, with very concave dorsal valves (?=8. Gerardi).” It was 
 subsequently shown,} through specimens obtained by Prof. A. Liversidge from the Darr 
 River,t that the two species were in all probability distinct, a point which 1 think now 
 capable of proof. In contradistinction to 8. Clarkei, the valves of S. Gerardi are both 
 densely spined ; the dorsal valve always very concave; the form more irregular in 
 outline and smaller, the area wide, short, and triangular; spines long, pendent, and 
 adpressed to the shell ; and the surface of both valves very concentrically frilled; but 
 particularly noticeable amongst these are the concave dorsal valves, and the short, high 
 triangular area in the ventral valve. 
 
 The internal structure of the dorsal valve has always been wanting to complete 
 the comparison, but this is now supplied by a Tasmanian specimen in the Australian 
 Museum, which I believe to be this species. The broadly oval forms of the renal or 
 vascular impressions resemble those of 8. Olarke?, rather than S. Jukesii, whilst, on the 
 contrary, the short septum indicates a resemblance to the latter. The deep depressions 
 on each side the septum in 8. Clarkei are quite absent, so is the transverse ridge 
 separating the upper from the lower pair of these, and probably the support of the 
 adductor muscles. The concavity of the dorsal valve varies, to some extent, in different 
 individuals, but it is always very apparent. The hinge-line also varies in length, long 
 in some examples, short in others, although, as before stated, it never extends the whole 
 width of the shell. 
 
 It would appear, therefore, from the foregoing remarks that in the Permo 
 Carboniferous rocks of this Continent and Tasmania, at least three species of Strophalosia 
 are met with, as originally described by the Writer. 
 
 The resemblance of the Australian examples of 8S. Gerardi to Prof. King’s 
 Indian type is very marked, both in outward shape, nature of the spines, form of the 
 dorsal valves, and the area. 
 
 * Proc. R. Phys. Soc. Edinb., 1880, v., p. 295. 
 
 + Journ. R. Soc. N. 8. Wales for 1883 [1884], xvii., p. 87. 
 + Locality doubtful. (R.Z.J.) 
 
262 
 
 Loc. and Horizon. Pelican Creek, Bowen River, five miles north of Sonoma 
 Station ; the same, opposite Palmer’s Old Station ; Parrot Creek, Bowen River, eight 
 miles up; Bowen River, between Traverse Stations 25 and 26 (R. L. Jack); Banana 
 Creek (H. W. Mackay; Colln. de Vis)—Middle or Marine Series, Bowen River Coal 
 Field ; “Darr River,* about three hundred miles south-west of Port Denison” (Prof. 
 A. Se oka ge; Colln. Sydney University). 
 
 Genus—CHONETES, Fischer, 1837. 
 (Oryctographie Gouy. Moscou., p. 134.) 
 
 CHONETES CRACOWENSIS, Etheridge, Pl. 18, fig. 9. 
 
 Chonetes cracowensis, Etheridge, Quart. Journ. Geol. Soc., 1872, xxvili., Pt. 3, p. 336, t. 18, f. 2. 
 Laguessiana, De Koninck, Foss. Pal. Nouv. alles du Sud, 1877, Pt. 3, p. 207, t. 10, f. 7 (excl. ES: 
 ‘5 99 Etheridge fil., Cat. Australian Foss., 1878, p. 48. 
 
 Sp. Char. Shell transversely oblong or semicircular, wider than long, both 
 valves ornamented with many ribs; hinge-line straight, not so long as the width of the 
 shell; area narrow and parallel; ventral margin convex. Cardinal angles rounded and 
 flattened at their extremities. Ventral valve slightly convex. Dorsal valve nearly flat, 
 or following the curve of the ventral. Beak small, apparently slightly incurved, but 
 not covering the hinge-line. The place of the hinge-spines faintly traceable. The 
 surface of the shell covered by what must have been short and stout spines numerously 
 distributed. (theridge.) 
 
 Obs. Mr. Etheridge considered that his species differed from the typical 
 Carboniferous Chonetes hardrensis (= C. laguessiana), De Koninck, by possessing 
 flatter cardinal angles, and many more spines. On the other hand, Prof. De Koninck 
 united ©. cracowensis with his C. laguessiana, and guided by his universally accepted 
 high opinion, I followed a similar course in the ‘“ Catalogue of Australian Fossils.” 
 But an examination of numerous specimens from the Star River Beds causes me to 
 doubt the advisability of this course, especially when Mr. Etheridge’s figure, which 
 excellently represents his species, is compared with that given by Prof. De Koninck of 
 the shell from New South Wales. The figure of C. cracowensis represents a form with 
 flat roundly rectangular sides, whereas the so-called C. laguessiana figured by De 
 Kouinck has acute cardinal angles, and the lateral margins rapidly and sharply merging 
 into the ventral margins. I quite fail to see how two such differently shaped shells can 
 be relegated to one species, and it will be better, in the meantime, to accept the name 
 applied by Mr. Etheridge to this shell. 
 
 Loc. and Horizon. Cracow Creek, Dawson River, Lat. 25° 20’ S., Long. 
 150° 15’ E., approximate (The late R. Daintree)—Middle or Marine Series of the Bowen 
 River Coal Field; Athelstane Range, Rockhampton (The late James Smith)—Gympie 
 Beds ; Corner Creek, Great Star River (R. L. Jack)—Star Beds. 
 
 > 
 
 CHONETES, sp. ind. (a.), Pl. 18, fig. 10; Pl. 87, figs. 21 and 22. 
 
 Obs. A transversely semicircular, deep, and very convex, or, in fact, almost 
 deltoid species, occurs in the Corner Creek Beds. It possesses the general form of 
 Chonetes polita, McCoy,t but, unlike the latter, is strongly costate. The alar angles 
 are pointed, and it is altogether an elegant little shell. 
 
 
 
 * In this, as in the case of Productus brachytherus, I doubt the correctness of the locality quoted, as 
 the Darr River is wholly in the Rolling Downs Beds. (R.L..J.) 
 + Davidson, Mon. Brit. Carb. Brach., 1861, Pt. 4, p. 190, t. 47, f. 8-11. 
 
 ~ 
 
263 
 
 In the Keelbottom River Series a somewhat similar shell is found, but less 
 convex, and very strongly ribbed, with the hinge abou equal in length to the shell. The 
 ribs are coarse and bifurcate, about thirty-five previous to division, and irregularly rounded. 
 
 It is quite possible that both these shells are one species, but in the presence 
 of the immense number of Chonetes already described, it is impossible to venture on 
 a name, especially when dealing with imperfect material. 
 
 Lec. and Horizon. Corner Creek, Great Star River (R. LD. Jack); Gully rising 
 in cliff between two peaks on left bank of Keelbottoin River, north of old Plum-tree Inn 
 (R. L. Jack)—Star Beds. 
 
 CHONETES, sp. ind. (b.), Pl. 18, figs. 7, 8, and 13. 
 [Compare C. australis, McCoy, Prod. Pal. Vict., Dec. iv., 1876, t. 35, fig. 1.] 
 
 Obs. The present Chonetes differs wholly from either of the preceding. The 
 ventral valve is broad and semicircular, quadrate, deeper than wide, and very slightly 
 convex. The hinge-line was as long as the shell, and when perfect the alar angles 
 bluntly pointed, but, as a rule, they are broken. A moderately broad hinge appears 
 to have been present, and there are the remains of several well-developed hinge-spines. 
 There was a well-marked septum in both valves, and the inner surface highly pustulose, 
 and punctate. The surface bore numerous distinct bifureating ribs, and there is some 
 indication of their having been spinose. 
 
 This species is probably closely allied to Chonetes australis, McCoy. It is 
 certainly not C. laguessiana, as figured by De Koninck from New South Wales, and 
 it does not appear to be a large form of C. cracowensis. It is also advisable to 
 compare, in passing, Chonetes falklandica, Morris and Sharpe,* with which there is 
 again some resemblance. Except that it is a larger species, C. ¢Jlinoisensis, Worthen,t 
 would represent our shell, especially in the very large number of costs. The latter 
 are numerous, but less so than in C. falklandica, and coarser; they bifurcate high up on 
 the visceral region, and are prominent and bold, although not coarse. 
 
 Loc. and Horizon. Athelstane Range, Rockhampton (The late James Smith) ; 
 Stony Creek, Stanwell, near Rockhampton (The late James Smith)—Gympie Beds. 
 
 CHONETES, sp. ind. (c.), Pl. 37, fig. 20. 
 
 Obs. A small, very flat shell, the ventral valve slightly elevated below the umbo, 
 then depressed in the middle line, producing a broad and very flat sinus. The hinge- 
 line as long as the shell, and the alar expansions also apparently flattened. The area is 
 small, and the septum extends for about half the height of the valve. The ribs are very 
 numerous and fine, and each one bifurcates ; they must have been provided with regular 
 concentric rows of spines, as the depressions representing the actual ribs are regularly 
 so pitted. The lateral ribs are much curved outwards, whilst the umbo was very fine 
 and small. 
 
 This pretty little cast at times looks more like an Orthotetes or Streptorhynchus, 
 than a Chonetes. The tripartite division of the surface probably arises from a rather 
 flatly prominent central region, and flattened alar expansions 
 
 This is evidently not far removed from Chonetes compressa Waagen,t and, in 
 
 fact, differs chiefly in the alar regions, being delicately striate, instead of quite plain. 
 Waagen’s remarks apply well to our specimens, bearing in mind that his examples were 
 perfect, comparatively speaking, whilst ours are only impressions. He says—‘‘ This is a 
 
 * Quart. Journ, Geol, Soc., 1846, ii., p. 274, t. 10, f. 4. 
 
 + Illinois Geol. Report, 1868, iii., t. 15, f. 8. 
 
 t Pal. Indica (Salt Range Fossils), 1884, Ser. xiii., Vol, i., No. 4, fase. 4, p, 680, figs. a-d, 
 
264 
 
 rather small species, with very flat valves, which are so close together that scarcely any 
 room remains between them. The ventral valve bears, in the middle, a low sinus, and 
 the radial striation of both valves is limited to the median parts, whilst the lateral parts 
 remain entirely smooth.” 
 
 Loc. and Horizon. Gully rising in cliff between two peaks on left bank of 
 Keelbottom River, north of Old Plum-tree Inn (2. LZ. Jack)—Star Beds. 
 
 CHONETES, sp. ind. (d.), Pl. 87, fig. 19. 
 
 Obs. A somewhat large, elongately quadrate, convex, and high cast occurs in the 
 fossiliferous masses of Mount Britton. There is a large wide area, deep sinus in the 
 dorsal valve of casts, and at least four hinge-spines on each side the umbo. The front 
 and sides are densely pitted, but the nature of the surface is unknown. 
 
 This form is only known to me as casts, but probably, judging from its size, is 
 allied to the Athelstane Range species (Pl. 18, fig. 8). The septum of the dorsal valve 
 was large and strong. The cardinal muscular scars of the ventral valve were small and 
 pear-shaped, and in this valve a septum also existed. 
 
 Loe and Horizon. Richards’ Homestead, three miles south-west of Mount Britton 
 Township (4. L. Morisset)—Middle or Marine Series of the Bowen River Coal Field. 
 
 Order—CLISTENTERATA. 
 Family—LINGULIDA. 
 
 Genus—LINGULA, Brugquiére, 1791. 
 (Encyclop. Méthod., i., Pl. 250, f. 1a-c.) 
 
 Lineuta mytinorpes, J. Sowerby, ? Pl. 18, fig. 19. 
 Lingula mytilloides, J. Sby., Min. Con., 1813, i., p. 55, t. 19, f. 1 and 2. 
 a mytiloides, Davidson, Mon. Brit. Carb. Brach., 1861, Pt. 4, p. 207, t. 48, f. 29-36. 
 
 Obs. Except that the specimen referred to this species is rather more angular 
 along the middle line of the valve, it is difficult to distinguish it from typical examples 
 of LZ. mytiloides. The test is preserved over half the surface of the specimen. Dana, 
 in his Work on the Geology of the Wilkes Expedition, describes a species, Lingula 
 ovata, which may perhaps also be the present shell. It is “quite small, much 
 convex, regularly broad ovate, with the front margin not at all truncate. Beak acute, 
 valves thin, smooth, with faint concentric lines of growth.” 
 
 The genus Lingula is of so scarce an occurrence in Australian Permo- 
 Carboniferous rocks that the present specimen is of some importance. 
 
 Loc. and Horizon. Spring Creek, Cania, Burnett (W. H. Rands)—Gympie 
 Beds. 
 
 Section—MOLLUSCA VERA. 
 Class—PELECYPODA. 
 
 Order—OSTRACEA. 
 Family—PECTINID ©. 
 Genus—EHNTOLIUM, Meek, 1872.* 
 (Hayden’s Final Report E. Nebraska, p. 189.) 
 
 Obs. The existence of this, as an Australian genus, depends upon a few small 
 and ill-preserved specimens in the Star River collections, made by my Colleague, and 
 
 * Prof. James Hall says—‘‘ Pal. California, 1864, i, App. B., p. 478,” and that Zntoliwm in its 
 Paleozoic sense is but a synonym of Pernopecten, Winchell. See Pal. N. York, 1885, v., Pt.1, No. 2, p. Wit. 
 
 
 
 
 
265 
 
 resembling the characteristic British species HZ. Sowerbii, McCoy, sp. One specimen 
 showed the concentric close ornament, and seems to be the valve with the conate ears ; 
 another displays the interior of the flat-eared valve (Pl. 14, fig. 10), and, above all points, 
 the typical central cartilage pit, the sockets for the obliquely diverging ridges, and the 
 long posterior lateral grooves; and there is a trace of the large eccentric adductor 
 muscular impression. | 
 
 These Corner Creek specimens are small, but bear no comparison with the 
 E. Sowerbii ; it is therefore, probably, a distinct and smalier species, but the material 
 is not copious enough to permit of a satisfactory determination. 
 
 Loe. and Horizon. Corner Creek, Great Star River (R. LZ. Jack)—Star Beds. 
 
 Genus—EUCHONDRIA, Meek, 1874. 
 (American Journ. Sci., 1874, vii., pp. 445 and 488.) 
 
 Obs. In this genus of Pectenoid shells, the hinge structure is peculiar. There 
 is a “comparatively large, oblique, central cartilage pit, and a row of smaller ones crossing 
 the area at right angles all along, both before and behind the large oblique central pit.”’ 
 
 The above are the late Professor F. B. Meek’s remarks in establishing his genus 
 for the little Pecten neglectus, Geinitz, from Illinois. He believed Euchondria to be 
 more nearly allied to Pernopecten, Winchell,* than to Aviculopecten, but differs from 
 the former in the obliquity of the central cartilage pit, and the presence of the true 
 eartilage pits along the hinge. The so-called cartilage pits along the hinge of 
 Pernopecten are probably only interlocking crenulations of the hinge, and not receptacles 
 for any portion of the ligament. 
 
 Amongst the many indistinct fossils from the Corner Creek Beds, was a small 
 semicircular shell with close, fine, concentric strix, a very rounded ventral margin, a 
 long hinge-line, anda small anterior ear with radiating ridges. Along the latter are 
 faintly visible the impressions of a vertical series of hinge-pits resembling those of 
 Euchondria. No central oblique pit was observed, however, and since the specimen has 
 passed from my hands, it has struck me that the genus Crenipecten, Hall,f might put 
 in as good a claim for it as Huchondria. In Hall’s genus the “hinge is furnished 
 with a series of small cartilage pits throughout its entire length”; and it would not 
 surprise me to find that the impression under discussion is more properly referable 
 to this than to the genus to which I assigned it in the list originally forwarded to my 
 Colleague.t 
 
 Loc. and Horizon. Corner Creek, Great Star River (R. LZ. Jack)-—Star Beds. 
 
 Family—A VICULOPECTINID:.§ 
 - Genus—AVICULOPECTEN, McCoy, 1851. 
 (Ann, and Mag. Nat. Hist., 1851, vii., p. 171.) 
 
 Obs. In the Corner Creek Beds, three species of Aviculopecten have been 
 noticed. In the first species the hinge-line is long, the surface covered with fine 
 radiating coste, and the anterior ear very pronounced, narrow, long, and triangular, with 
 
 
 
 * As a matter of fact it is more nearly allied to Crenipecten, Hall. 
 
 + Prelim. Notice Lamellib. Shells, Up. Helderberg, Hamilton and Chemung Groups, Pt. 1, 1884, 
 p. 406d, 
 
 + Handbook Queensland Geol., 1886, p. 39. 
 
 § Meek and Hayden, Pal. Up. Missonri, 1865, Pt. i., p. 49 
 
266 
 
 three or four strong diverging ridges. The second species is highly cancellate, the 
 radiating coste being fine, close, and round. ‘The third shell is very small, and indicates 
 a triangular species very narrow towards the umbones, and widening ventrally. No 
 ornament is preserved, and only one of the anterior ears, which is triangular and deeply 
 divided from the body of the shell. The whole of these points are such common 
 characters amongst this group of shells, that they cannot be alone used for specific 
 differentiation. 
 
 Mr. Rands has collected from Banana Creek, near Rockhampton, what is obviously 
 another fragment of an Aviculopecten. It is a fragment without ears or hinge-line, 
 covered with fine, elevated, radiating striz, slightly curved towards the sides of the shell, 
 and with an intermediate rib between each pair; the whole are crossed by equidistant 
 regular concentric lines, forming, by their intersections, small quadrangular spaces. 
 
 AVICULOPECTEN SUBQUINQUELINEATUS, McCoy, sp. 
 
 Pecten comptus, Dana (non McCoy), American Journ. Sci., 1847, iv., p. 160. 
 
 3 subquinquelineatus, McCoy, Ann. and Mag. Nat. Hist., 1847, xx., p. 298, t. 17, f. 1. 
 
 », comptus, Dana, Geology Wilkes’ U. S. Explor. Exped., 1849, Vol. x., p. 704, Atlas, t. 9, f. 5. 
 
 » subquinquelineatus, McCoy, Proc. R. Soc. V. D. Land, 1851, i., p. 322, t. 17, f. 1. 
 Aviculopecten subquinquelincatus, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 8, p. 295, t. 22, f. 2 
 
 » A Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 297, t. 15, £. 52. 
 Obs. This is a large, strong, and distinctly marked species, at first sight 
 resembling A. Fitton, Morris,* but easily distinguishable from it by the plain and entire 
 condition of the radiating cost ; whereas in A. Fittoni the latter are composed of a 
 series of smaller radii. In both species the valleys between the ribs are filled with 
 subordinate coste. In Morris’s species there is only one between each pair of ribs, but 
 in McCoy’s there are from three to five. In A. swbquinquelineatus the ears are large 
 and radiately striated, and the whole shell must have grown to some considerable size. 
 It appears Professor Dana’s name of P. comptus has precedence of McCoy’s by a short 
 time, and would be the accepted one for this species, were it not that the name comptus 
 had already been used by Professor McCoy + for an Irish Carboniferous Limestone shell. 
 Professor Dana’s name has therefore to give way to the subsequently described 
 P. subquinquelineatus. 
 Loc. and Horizon. Bowen River, at No. 25 Traverse Station (R. L. Jack), in 
 
 a hard flinty micaceous sandstone of the Middle or Marine Series, Bowen River 
 Coal Field. 
 
 AVICULOPECTEN LIMHFoRMIs, Worris, ? Pl. 14, fig. 1. 
 Pecten limeformis, Morris in Strzelecki’s Phys. Descrip. N.S. Wales, &c., 1845, p. 277, 6. 18, f. 1. 
 Aviculopecten limeformis, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 291, t. 22, f. 4. 
 ae sp. nd., Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 298. 
 
 Obs. A single specimen of a large species of Aviculopecten, with portions of the 
 valves in apposition, has been obtained by my Colleague. It is a mere cast with remains 
 of shelly matter here and there, but appears to correspond to a great extent with A. 
 limeformis, Morris.{ The shell is very inequivalve, one valve being moderately convex, 
 the other almost flat, or even, towards the ventral margin, a little concave. These 
 characters would accord better with those of the species mentioned, than with any other 
 of the Australian forms so far as described to the present time. In the Daintree 
 Collection, Mr. Etheridge determined the presence of this shell and gave the following 
 
 
 
 * Strzelecki'’s Phys. Descrip. N. S. Wales, &c., 1845, t. 14, f. 2. 
 + Synop. Carb. Limest. Foss. Ireland, 1844, p. 90, t. 15, f. 14. 
 {Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 277, t. 13, fig. 1. 
 
267 
 
 diagnosis * :—‘ Shell inequilateral or oblique, slightly convex near the umbonal region 
 or beak ; the ribs are also irregular and wavy, about thirty-five in number, and all meet 
 near the umbo ; lines of growth obscurely wrinkled ; ears small, radiated, and coarsely 
 wrinkled. Prof. Morris does not state the dimensions of his shell; proportionately our 
 single specimen agrees with his, but apparently is individually larger.” 
 
 The general obliquity of the valve, and the convexity in the umbonal region, 
 certainly point to this species, but the anterior ear, well relieved from the body of the 
 shell, does not accord at all with Morris’s figure, nor is there any indication of this in 
 De Koninck’s illustration. I must confess to never having seen a complete individual 
 of this species, and I am therefore rather in the dark as to its true appearance ; but 
 the obliquity, and the great inequality of the valves, as expressed above, are certainly 
 important characters. 
 
 I now figure a rather similar Avicwlopecten (PI. 14, fig. 1) from Gympie, in which 
 the anterior ear is similar in shape to that of Mr. Etheridge’s figure, but is less detached 
 from the shell. This, for the present, must be regarded as referable to A. limeformis. 
 
 It is so rare to obtain any of these Australian Aviculopectens with the true shell 
 remaining that identification in such a case, especially with mutilated examples, becomes 
 difficult. Such a specimen has been obtained in the Yatton Gold Field, but space does 
 not permit of our figuring it. The valves are in apposition, and portions of the ears 
 wanting. The larger valve is oval and decidedly convex, the smaller convex in the 
 visceral region, but gradually becoming flat, or even concave towards the front margin, 
 and to some extent also, the sides. In these we trace decided A. limeformis characters. 
 Both valves possess about twenty-four broad, rather flattened ribs, those of the one 
 valve fitting into those of the other at the ventral margin, and causing the latter to 
 become fluctuating. Corresponding interspaces exist crossed by very close projecting 
 frills. One end of the shell (itis difficult to say which, the ears being removed) is convex 
 in the larger valve, but sublobate in the flat or concave piece, another character of 
 A. limeformis. 
 
 Until the entire appearance of the last-named is more familiar, the identity of 
 these species must remain open, but if not A. limeformis, it is possible that the present 
 form, and Mr. Etheridge’s figured specimen, may form a separate species, as they appear 
 to have several points in common. 
 
 Loc. and Horizon. Coral Creek, Bowen River, below Sonoma Road-crossing 
 (Rh. L. Jack) —Middle or Marine Series, Bowen River Coal Field ; ? Gympie (2. L. Jack) 
 —Gympie Beds; ? Yatton Gold Field (R. L. Jack)—Gympie Beds. 
 
 AVICULOPECTEN ? IMBRICATUS, Htheridge. 
 
 Aviculopecten ? imbricatus, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 326, t. 14, f. 2. 
 ns a Etheridge fil., Cat. Australian Foss., 1878, p. 6. 
 
 Sp. Char. Shell inequilateral, and possessing twenty-two ribs, the ends or 
 extremities of which imbricate or overlap in the cast; there appears to be, or to have been, 
 a space between the end of each rib at its extremity, or along the ventral margin ; 
 faint longitudinal markings run down each of the ribs, following their course. 
 (Ltheridge.) 
 
 Obs. An impression only occurs, and that of the inner surface, of one valve 
 of this singular and doubtful shell. Our figure is taken from a gutta-percha cast of 
 the impression left. That it belongs to the Asiphonida I do not doubt, and, I believe, 
 
 
 
 * Quart. Journ. Geol. Soc., 1872, xxviii., p. 326, t. 14, f 1. Iam much puzzled by the central oval 
 impression on the umbonal region. It cannot be a cartilage pit of the hinge, as it is in the wrong position 
 for such a structure. (R. ZL., jun.) 
 
268 
 to one of the Aviculide. The umbonal region is certainly not complete ; and, 
 therefore, no true conclusion can be arrived at relative to the nature of the ears and 
 hinge-line of the perfect shell. (Htheridge.) 
 Loc. and Horizon. Gympie (Lhe late R. Daintree)—Gympie Beds. 
 
 AVICULOPECTEN MULTIRADIATUS, Htheridge. 
 Aviculopecten multiradiatus, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 327, t. 18, f. 1. 
 
 Sp. Char. Shell nearly equilateral, orbicular, depressed, slightly convex, with 
 about sixty well-defined equidistant sharp ribs, all meeting at the umbo; these ribs 
 appear to have been sharply elevated and plain; ears not seen; lines of growth well 
 defined. (Htheridge.) 
 
 Obs. Aviculopecten multiradiatus was compared by Mr. Etheridge to A. plano- 
 radiatus, McCoy, and A. docens, McCoy, both species of the British Carboniferous 
 Limestone. It differs from the first in being less convex, but appears to be a more 
 robust shell than the latter. The Author likewise added— It has also affinity with 
 Pecten squamuliferus, Morris, from Mount Wellington, Van Diemen’s Land.* I 
 cannot, however, clearly determine the presence of imbricated scales upon the ribs.” 
 Unfortunately, in the figure accompanying these remarks, the indications of scales on 
 the ribs are distinctly visible, and it is exceedingly probable that the shell is only, after 
 all, Aviculopecten squamuliferus, Morris. 
 
 Loc. and Horizon. Gympie (The late R. Daintree)—Gympie Beds. An 
 Aviculopecten like this species also occurs at Kooingal (Zhe late James Smith)— 
 Gympie Beds. 
 
 AVICULOPECTEN LAURIENTI, sp. nov., Pl. 43, figs. 3 and 4. 
 
 Sp. Char. Shell small, orbicular, sub-equilateral, anterior, posterior and ventral 
 margins rounded; umbones small, moderately acute. Right valve hardly convex, much 
 flattened ; anterior ear elongately triangular, narrow,. separated by a long, deep, and 
 narrow byssal sinus; posterior ear small, more or less rectangular; surface smooth, or 
 with a few concentric growth-marks ; ears apparently smooth. Left valve slightly convex, 
 with a straight hinge-line, rather less than the width of the shell, squarish ; anterior ear 
 small, triangular, posterior small but wing-like; anterior ear and body of the valve 
 covered with a large number of very fine radiating coste and interpolated riblets, crossed 
 by equally fine concentric decussating lamine, and especially well marked on the anterior 
 ear. 
 Obs. It is impossible to admit the shell De Koninck has ealled Avieulopecten 
 depilis,+ to McCoy’s species of the same name. It is probable that the present shell is that 
 referred to by the former under that designation. In A. depilis, McCoy, the anterior 
 ear of the right valve is squarish, not particularly elongated, and but little separated 
 from the shell. In the present species it is quite the opposite of this. Had these 
 characters been applicable to the left, instead of the right valves, a very close resemblance 
 would have existed between the fossils now before me and A. variabilis, McCoy.§ On 
 the whole I think it will be better to separate them under the above name rather than 
 admit a doubtful reference to a little known European species. I name this in memory 
 
 of Prof. L. G. De Koninck. 
 
 * Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 278, t. 14, f. 1. 
 + Foss. Pal. Nouvy.-Galles du Sud, 1877, Pt. 3, t. 22, f. 7. 
 
 + Synop. Carb. Limest. Foss. Ireland, 1844, t. 16, f. 11. 
 
 Sel iidaabalamesid s 
 
269 
 
 Loe. and Horizon. West of the Dividing Range, at the Crow’s Nest, Mount 
 Victoria, near Mount Morgan (The late James Smith; Mining and Geol. Mus., 
 Sydney) ; Rockhampton District * (C. W. De Vis; Colln. De Vis) —Gympie Beds. 
 
 Genus—DELTOPECTEN, gen..nov. 
 
 Gen, Char. Shell possessing the general structure of Aviéculopecten, but the 
 valves very inequivalve, the larger or convex valve with a high overcurved umbo, 
 overhanging a long triangular hinge area, with longitudinal cartilage furrows, and a 
 large deltoid-triangular cartilage pit. 
 
 . Obs. Deltopecten is intermediate in its structure between Pecten and 
 Aviculopecten. It possesses the central cartilage pit of the former, and the furrowed 
 area of the latter, and besides this the larger or convex valve is much higher 
 than its neighbour, the umbo of the one overhanging that of the other, similar to the 
 structure of the genus Janira. It may therefore be said to be a compound of the 
 structure of all three genera. This so thoroughly departs from the structure of 
 Aviculopecten, and is, further, such an additional modification of the hinge structure in 
 this group of shells, to that indicated cf late by various American Authors, that it seems 
 to me to be worthy of generic distinction. I therefore propose for the following 
 Australian species, the only one in which I have as yet noticed this structure, the 
 name Deltopecten, in allusion to the shape of the cartilage pit or depression occupying 
 the hinge area. 
 
 Type. Pecten illawarensis, Morris. 
 
 DELTOPECTEN ILLAWARENSIS, Morris, sp., Pl. 41, fig. 3; Pl. 43, fig 2. 
 
 Peston illawarensis, Morris in Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 277, t. 14, f. 3. 
 fe Dana, Geology Wilkes’ U.S. Explor. Exped., Vol. x., 1849, p. 705, Atlas, t. 9, £..9. 
 A yeaitonenten ulawarensis, De Koninck, Foss. Pal. Nouv.-Galles du Sud, Pt. 3, 1877, p. 301, t. 22, f. 1. 
 
 Obs. Prof. De Koninck has correctly described this shell as inequivalve, even 
 allowing for the fact that nearly all shells of this group are more or less so. The 
 larger valve is very much the more convex of the two, and better developed, with a large 
 and high umbo overhanging the hinge area. These points are well shown in De 
 Koninck’s figures. The area is exceedingly broad and strong, especially beneath the 
 umbones, where it is excavated into-a pseudo-cartilage pit of a deltoid or roundly 
 triangular form, the area gradually narrowing outwards towards the anterior and 
 posterior extremities. The pit must have been the receptacle for a large and strong 
 cartilage. The whole area is coarsely transversely striated, or grooved. 
 
 The radiating cost of the surface vary to some extent in number. In Prof. 
 Morris’s figure, which appears to be that of the smaller valve, there are twelve or thirteen 
 ribs, in that given by De Koninck of the same valve fifteen, whilst his view of the 
 convex valve exhibits still more, perhaps twenty. In our specimens, the average 
 number appears to be about fourteen. 
 
 The depression of the valves towards the front margins, referred to by De 
 Koninck, takes place between the edges and the pallial impression, which is a well- 
 marked feature in the examples before me. 
 
 In Professor James Hall’s figure of Aviculopecten princeps, Conrad, sp.,¢ there 
 is both a triangular area, and a central depression. The former is very apparent, 
 
 
 
 
 
 * See note, p. 199. 
 + Prelim. Notice Lamellib. Shells, Up. Helderberg, Hamilton and Chemung Groups, Pt. 1, 1884, 
 
 6.2, f. 4, 
 
270 
 
 but the latter is but indistinctly outlined. It is possible that a re-examination of this 
 species, with the light thrown by D. il/awarensis, may show a closer relation between 
 the two. 
 
 Loe. and Horizon. Richards’ Homestead, three miles south-west of Mount Britton 
 Township (Ze. Hull)—Middle or Marine Series, Bowen River Coal Field. 
 
 Genus—PTERINOPECTEN, Hail, 1884. 
 
 Pterinopecten, Hall, Pal. N. York, 1884, v., Pt. i., No. 1, p. xii. 
 a 35th Ann. Report, Regents Univ. State Cab. N. York, 1884, p. 406d. 
 
 Gen. Char. General characters of Aviculopecten, but the hinge-line long. Lars 
 not well defined, being simple expansions or extensions of the upper lateral margins to 
 the hinge-line. Test ornamented with rays. (Hail.) 
 
 Obs. Prot. Hall is, I believe, quite correct in separating from <Aviculopecten 
 those forms in which the ears are ill-defined, and not cut off from the body of the 
 shell, especially the anterior one, except in one valve, as is usually the case in the typical 
 species of that genus. This is accompanied by a posterior obliquity of the shell, which 
 is equally characteristic. I have not Sowerby’s ‘‘ Mineral Conchology ”’ to refer to, but if 
 memory does not deceive me, Pecten papyraceus, Sby., of the English Coal Measures, 
 will fall into this genus. Perhaps also Aviculopecten nodulosus, De Koninck,* will form 
 another species. 
 
 PrertnorpecteN DeEvistI, sp. nov., Pl. 40, fig. 9. 
 
 Sp. Char. Shell of medium size, obliquely rhomboidal, the length and height 
 being nearly equal, but the greatest length a little below the middle. Anterior 
 and ventral margins regularly rounded, but the posterior margin sigmoidally curved. 
 Hinge-line straight, a little shorter than the length of the shell. Umbonal region 
 more or less flattened ; beaks inconspicuous, anterior. Anterior ears small, triangular, 
 separated by an undefined sulcus; posterior ears flattened, margins concave, and their 
 extremities pointed. Surface of the left valve with moderately strong, direct, and non- 
 flexuous radiating coste, becoming much finer on the posterior ears, those on the 
 body of the shell, at least, bifurcating, perhaps all; concentric lines of growth wide 
 apart. 
 
 Obs. There is a strong resemblance between all the species of this genus, and it 
 is at times difficult to differentiate between them. The present species is, however, a 
 marked one, from the relative resemblance between the height and length. In general 
 outline P. Devisti approaches very closely the British Coal Measures species, P. papy- 
 raceus, Sby., sp., but is more coarsely ribbed. In outline there is a marked correspondence 
 with P. hoosacensis, Wallcott,+ but a similar difference exists here, in addition to the 
 fact that the ribs are less numerous. In the extensive height of its valves, our species 
 is also very like P. erectus, Hall, of the Chemung Group of North America. 
 
 It is named in honour of Mr. C. W. De Vis, M.A., Curator of the Queensland 
 Museum, to whom I am indebted for numerous contributions of specimens for the 
 illustration of the present Work. 
 
 Another specimen, from the same Collection, with the umbones and hinge-line 
 wanting, closely resembles the type specimen in general appearance, but the radiating 
 coste are much finer, and far more numerous. They are also nodulated, but whether 
 
 
 
 * Faune Calc. Carb. Belg., 1885, Pt. 5, t. 37, f. 6. 
 + Mon. U.S. Geol. Survey (Pal. Eureka District), 1884, viii., p. 232, t. 8, f. 9. 
 
271 
 
 independently, or as arising from the passage of concentric lamin, it is impossible to 
 say. It is, of course, conceivable that this may represent a distinct species resembling 
 very closely the British P. papyraceus. 
 Loc. and Horizon. Rockhampton District * (0. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 Order—MYTILACEA. 
 Family—A VICULID. 
 
 Genus—MERISMOPTERTIA,* gen. nov. 
 
 Gen. Char. Pteronitiform in appearance, the anterior end lobe-like and well 
 developed ; posterior end alate. Area excavated along the cardinal edge of both valves, 
 and deeply ridged for the reception of a ligament; cardinal teeth wanting, but a strong 
 clavicle descends in each valve before the anterior adductor muscles; one or more lateral 
 teeth in each valve. Anterior muscular scars double and strong, the superior scar situated 
 towards the umbones. External ornament of concentric ridges. 
 
 Obs. Those acquainted with Pterinea will at once perceive that the shell so 
 generally known to Australian Paleontologists as Pterinea macroptera cannot properly 
 be referred to that genus, from the character of its hinge. In Pterinea there are well- 
 defined cardinal teeth, anterior in position to the umbones, and one or more posterior, 
 lateral, oblique teeth, besides a striated or grooved hinge-margin, and a well-developed 
 posterior muscular scar. In the proposed new genus, there are no cardinal teeth proper, 
 one lateral tooth only, either oblique or horizontal, and, further, the posterior scar is 
 very indistinctly developed. But, proceeding from the cardinal margin, and anterior to, 
 and bounding the anterior scar, is a very strong clavicle or crest, leaving very deep slits 
 in casts. Herein the structure of this shell differs very widely from that of Pterinea. 
 The hinge area of each valve is large, high, and coarsely ridged, and when the valves are 
 in apposition, forming a deep angular and elongated depression, which, during life, must 
 have been filled by a strong and powerful ligament. 
 
 These features are particularly well shown in Morris’s figure of P. macroptera, 
 especially the clavicle and the posterior lateral tooth. In Prof. De Koninck’s figure, on 
 the other hand, the anterior scar is placed before the clavicle, a very erroneous repre- 
 sentation, as it succeeds immediately after it, and is supplemented by a very prominent, 
 but at the same time smaller scar above it towards the umbones, but still not within 
 the beak cavity ; this scar is not shown in De Koninck’s figure at all. 
 
 Type. Pterinea macroptera, Morris. 
 
 MERISMOPTERIA MACROPTERA, Morrvs, sp. 
 
 Pterinea macroptera, Morris in Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 276, t. 18, f. 1 and 2. 
 De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 305, 
 rp oP Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 298. 
 
 Obs. My Colleague has obtained a Pterinea, clearly this species, but only one 
 specimen, and that without a part of the posterior wing. The small anterior lobe is 
 only partially preserved ; the hinge-line was clearly somewhat less than the width of 
 the shell; and there are distinct remains of concentric lamine, although the specimen 
 is only a cast. The cast of one of the characteristic teeth is also preserved. 
 
 Loc. and Horizon. Coral Creek, below Sonoma Road-crossing, Bowen River 
 (R. L. Jack)—in decomposed nodular ironstone of the Middle or Marine Series of the 
 
 Bowen River Coal Field. 
 
 ” ” 
 
 
 
 * See note, p. 199. 
 + PEepio.0s = a partition. 
 
272 
 
 Family—MYTILID. 
 
 Genus—MYTILOPS, Hall, 1884.* 
 (Pal. N. York, v., Pt. 1, No. 1, p. xiv.) 
 
 Myrrnors ? CORRUGATA, sp. nov., Pl. 40, fig. 11. 
 
 Sp. Char. Shell obliquely mytiliform, triangular, produced more or less pos- 
 teriorly and ventrally. Dorsal or cardinal margin short and straight, not obliquely 
 elevated ; ventral margin oblique, longer than the cardinal margin ; anterior end small, 
 somewhat puckered ; posterior margin obliquely truncated. Beaks terminal. Surface 
 with from twelve to twenty step-like imbricating flattened and concentric ridges, 
 non-striate, and graduating upwards to the umbones. Diagonal ridge broadly convex. 
 
 Ovs. This is a small shell, much resembling in its surface markings MeCoy’s 
 Pullastra ? striatocostata,t except that it is oblique, the hinge-line short, and the 
 concentric cost plain. In the latter, which has been figured by De Koninck { as 
 Edmondia ? striatocostata, the dorsal and ventral margins are parallel, and the ends 
 elliptically rounded. Here both are very oblique. The external markings give the 
 present shell a very noticeable appearance. I have not seen the nature of the hinge, 
 but it corresponds with the external characters of the shells named Mytilops by Prot. 
 James Hall. There is some resemblance between <Avicula Hurdii, De Koninek, 
 and the present species, but the latter is a much deeper shell. 
 
 Loc. and Horizon. Rockhampton District § (C. W. De Vis; Colln. de Vis)— 
 Gympie Beds. 
 
 Myvitops ?, sp. ind., Pl. 14, fig. 20. 
 [Compare Mytilus Bigsbyi, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, t. 21, f. 1.] 
 
 Obs. The shells described by De Koninck from New South Wales will probably 
 fall within Hall’s genus Mytilops. The present form is neither so thick nor yet so 
 transversely expanded as this species, otherwise it appears to be very near it. Only two 
 examples have come before me, both much compressed, and one imperfect. The nature 
 of the interior of the shell is unknown. 
 
 Loc. and Horizon. Gympie (2. L. Jack)—Gympie Beds. 
 
 Genus—MODIOMORPHA, Hall and Whitfield, 1869. 
 (Prelim, Notice Lamellibranc Shells, p. 72.) 
 
 Mopromorpua ? DaAtnrreet, sp. nov., Pl. 14, fig. 18. 
 
 Sp. Char. Shell transverse, elongately triangular, or irregularly subobovate, 
 narrowed anteriorly, expanded posteriorly ; probably thin-shelled ; a narrow ill-defined 
 sinus proceeds from the umbones to the ventral margin, immediately at the anterior end. 
 Hinge long but not extending the whole length of the shell, rising slightly posteriorly ; 
 ventral margin straight at the anterior end, rather curved posteriorly. Anterior end 
 small, lobate, posterior end subalate ; margin obliquely truncated. Anterior muscular 
 scars small, close under the umbones; beaks moderately acute; valves convex, with 
 strong diagonal ridges, the surface between them and the hinge more or less concave ; 
 ornament unknown. 
 
 
 
 * This genus may have been proposed at an earlier date, but it is very difficult to get at the real dates 
 of a large number of Prof. Hall’s genera, his system of publication being, to say the least of t, a very 
 complicated one. The above is the first reference I am acquainted with. (R. HZ, Junr.) 
 
 + Ann. and Mag. Nat. Hist., 1847, xx., p. 305, t. 14, f. 3. : 
 
 + Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 269, t. 18, f. 3. 
 
 § See note, p. 199. 
 
273 
 
 Obs. The present shell appears to correspond in general outline with those 
 American Bivalves for which Prof. James Hall and Mr. Whitfield have proposed the 
 above genus. There is, however, a less arcuate outline, and a more determinate diagonal 
 ridge. The concavity above the latter is a very marked feature in this species. Further- 
 more, I have not seen “the single strong wedge-form tooth in the left valve, and 
 corresponding cavity in the right,” which appears to distinguish Modiomorpha. 
 
 One specimen seems to show indications of some radiating ribs on the body of 
 the shell, parallel to the diagonal ridges, but they are very indistinctly preserved. 
 
 Loe. and Horizon. Hawkins’ Gully, Kroombit Diggings, Port Curtis (W. H. 
 Rands)—Gympie Beds. 
 
 MopioMorPHA MYTILIFORMIS, sp. nov., Pl. 14, fig. 5; Pl. 40, fig. 4. 
 
 Sp. Char. Shell transversely ovate, modioliform, convex, curved, moderately 
 gibbous, expanding posteriorly, dorsal and ventral margins divergent. Anterior end 
 small but non-lobate, its margin rounded. Posterior end expanded, gradually com- 
 pressed, the convexly rounded margin gradually passing imperceptibly into the dorsal 
 margin, the widest portion of the curve being above; ventral margin concave cen- 
 trally, convex anteriorly and posteriorly ; cardinal or dorsal margin elevated, nearly 
 straight but not in the least angulated; hinge-line of the left valve with a long socket 
 under the beaks for the reception of tooth of the opposite valve, and a long posterior 
 lateral tooth; valves convex medianally, a broad and rounded diagonal ridge proceeding 
 from the beaks and becoming lost towards the posterior end. Umbones small and quite 
 anterior, an almost imperceptible sinus running from them in each valve, to the ventral 
 margins. Surface with broad concentric folds. 
 
 Obs. This shell is very like the smaller figure of MeCoy’s Modiola crassissima,* 
 but not the larger one, and may even be the latter. But in the present shell there is 
 no angulation of the posterior hinge-line, this and the posterior margin insensibly 
 passing into one another. Again, there is little or no sulcus from the umbones towards 
 the ventral margin, the sinuation of the latter being much more gradual in the present 
 shell, and placed nearer the centre of the margin, with a corresponding decrease in 
 height of the posterior end. To some extent MW. mytiliformis resembles Cypricardia 
 imbricata, Dana,t but in the figure of the latter the ventral margin is not at all inflected, 
 and there does not appear to be any umbonal slope. Furthermore, the posterior end, 
 judging by the surface ornament, was sigmoidal. In. Pl. 88, figs. 12 and 13, is probably 
 represented the younger condition of this species, which is equally like Dana’s 
 Cypricardia prerupta,t but the cardinal margin of the latter is too horizontal; 
 and again there is an entire absence of the diagonal convexity visible in our little 
 shell. 
 
 The young form (PI. 38, figs. 12 and 13) again might at times be mistaken for 
 Dana’s Cypricardia simplex,§ but the same points will serve to separate the two. The 
 
 name Cypricardia is merely quoted from Dana, as it is most inappropriate to these 
 shells. 
 
 Loc. and Horizon. Banana Creek, Banana, Dawson River (2. L. Jack and 0. W. 
 De Vis) ; Richards’ Homestead, three miles south-west of Mount Britton Township 
 (R. Hull)—Middle or Marine Series, Bowen River Coal Field. 
 
 
 
 * Ann. and Mag. Nat. Hist., 1847, xx., p. 300, t. 15, f. 2 and 3. 
 
 + Geology Wilkes’ U. S. Explor. Exped., Vol. x., Atlas, t. 8, f. 5. 
 + Ibid., f. 10, 
 
 § Ibid, t. 9, £. 2. 
 
274 
 Order—ARCACEA., 
 ARCIDA. 
 
 
 
 Family 
 
 Genus—PARALLELODON, Meek and Worthen, 1866.* 
 (Proc. Chicago Acad., i., p. 17.) 
 
 PARALLELODON COSTELLATA, McCoy, Pl. 40, figs. 12 and 13. 
 Byssoarea costellata, McCoy, Synop. Carb. Lime. Foss. Ireland, 1844, p. 72, t. 11, f. 36. 
 Palearea costellata, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 286, t. 16, f. 6 and 7. 
 
 Sp. Char. Shell small, subrhomboidal, rather square-ended, valves fairly convex, 
 about twice as long as wide. Anterior end short, rather alate, the margin rounded, 
 joining the hinge-line at a sharp angle ; posterior end produced and compressed, the 
 margin obliquely truncated, and rather emarginate. Dorsal margin straight, as long as 
 the shell; ventral margin rounded, with a slight concavity a little anterior to the middle. 
 Diagonal ridge pronounced but not acute, posterior slope rather concave, a sinus 
 traversing the valves obliquely from the umbones to the concavity in the ventral 
 margin. Posterior teeth three, long and rather oblique. Surface with concentric 
 ridges at irregular intervals, close or distant, crossed by innumerable, fine, almost 
 microscopic, radiating striz, somewhat broken or fluctuating. 
 
 Obs. IT am unable to compare: this shell with McCoy’s figure, and have to 
 accept De Koninck’s determination, but the above description will serve to show the 
 trivial differences which exist between the present shell and the latter’s description. 
 These are the presence of the large number of radiating strie, and three instead of 
 two posterior teeth. In addition to these points the Queensland shell is much larger. 
 Possibly it is a distinct species, and in that case may be known as Parallelodon 
 Konineki. 
 
 Loc. and Horizon. Rockhampton District | (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 Family—NUCULIDZ. 
 
 Genus—NUCULA, Lamarck, 1799. 
 (Prodrome, p. 87.) 
 
 Nvcuwta, sp. ind., Pl. 40, fig. 10. 
 
 Obs. A cast of a small oblong-deltoid shell, with a short posterior hinge, and a 
 very abrupt, almost vertical, anterior margin. The anterior end is much reduced in size, 
 and the beaks quite terminal; the posterior end is curved and produced. There are 
 impressions of six hinge teeth, and traces of fine concentric striz. 
 
 This fragment is so far satisfactory, that it demonstrates the presence of the 
 genus in the Queensland beds. It properly belongs to the group of Nucula tumida, 
 Phill.t The cartilage pit has not been satisfactorily seen. 
 
 Loc. and Horizon. Rockhampton District § (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 * Macrodon, Lycett, 1845, non J, Miiller, 1842, 
 
 + See note, p. 199. 
 
 + Not to be confounded with WV, tumida, Ten, Woods, a South Australian Tertiary Shell, which 
 requires renaming. 
 
 § See note, p. 199, 
 
275 
 Family—NUCULANIDA, 
 
 Genus—NUCULANA, Link, 1807. 
 (Beschr. Natur, Samml. Rostok, iii., p, 155.) 
 
 Noucvnana, sp. ind., Pl. 14, fig. 17. 
 
 Obs. A small specimen of a very inequilateral Muculana represented by 
 an external impression, after the type of WV. leiorhynchus, McCoy,* and Nucula 
 birostrata, McCoy.+ It possesses a snout-like posterior end. The anterior was moderately 
 long, the umbonal region a good deal canted over to the posterior side, and high. The 
 posterior end is sharply pointed, with a strong posterior angle, and the body of the 
 shell delicately striate. It is absolutely impossible to distinguish between the present 
 shell and an undetermined Carboniferous Nuculana figured by Messrs. Meek and 
 Worthen but not described.{ Our specimen corresponds in every particular, even to 
 size, and although the material is too little to found a species on, I would beg to suggest 
 that in the event of further specimens showing the Queensland shell constant, that it 
 and the American species be called Nuculana Wortheni. 
 
 Loe. and Horizon. Corner Creek, Great Star River (R. ZL. Jack)—Star Beds. 
 
 Order—LUCINACEA. 
 Family—SOLEMYID. 
 
 Genus ~SOLEMYA, Lamarck, 1819. 
 Solemya, Lamarck, Hist. Nat. Anim. sans Vért., 1819, v., p. 488. 
 Janeia, King, Mon. Permian Foss. England, 1850, pp, 177 and 246, 
 Soremya EDELFELTI, sp. nov., Pl. 14, fig. 16. 
 
 Sp. Char. Sheil narrow-oblong, length two and a quarter inches. Hinge-line 
 not as long as the shell, a little angulated on the anterior side; beaks about one-third 
 from the anterior end, apparently a little depressed. Anterior end small; posterior 
 end elongated, possibly compressed; posterior slope small, and but slightly marked ; 
 posterior margin obliquely truncate. Surface with a large number of sharp, strong, 
 radiating ribs, distributed over the whole, with a few transverse corrugations. 
 
 Obs. This fine species is a worthy addition to the limited number of Solemye 
 known, and is named in compliment to the Collector. 
 
 In case it should at first sight be taken either for Plewrophorus costatus, Morris, 
 or P. Morrisit, De Kon., it may be at once distinguished by having the whole surface 
 radiate. 
 
 Loe. and Horizon. Stonehumpy Creek, Bowen River (#. Hdelfelt)—Middle 
 or Marine Series, Bowen River Coal Field. 
 
 Family—ASTARTID. 
 Genus—PLEUROPHORUS, King, 1844. 
 (Ann. and Mag. Nat. Hist., xiv., p. 313.) 
 PLEvROPHORUS Ranpst, sp. nov., Pl. 14, fig. 14. 
 Sp. Char. Shell oblong, moderately convex. Hinge-line straight and long; 
 ventral margin gently convexly rounded. Anterior end small, posterior end flattened, 
 
 * Synop. Carb. Lime. Foss. Ireland, 1844, t. xi, f. 27. 
 + Synop. Carb, Lime, Foss. Ireland, 1884, t. 11, f. 23. 
 t Illinois Geol. Report, 1878, v., t. 26, f. 10, 
 
276 
 
 the margin obliquely curved downwards, posterior slope not manifest; siphonal ridge 
 slightly perceptible. Umbones small, quite anterior, and from them proceed four diagonal 
 ridges, spreading out ventrally: surface otherwise concentrically lined. 
 
 Obs. The above characters are taken from a decorticated cast. From P. 
 Morrisii, De Koninck, this species differs by having diagonal ridges confined to the 
 centre of the valve. From P. biplex, De Koninck, by possessing four instead of two 
 diagonal ridges, as well as a much straighter hinge, and a different outline to the 
 posterior margin. P. Randsi is undeniably nearest to the European P. costatus, 
 Brown,* but in the latter the divaricating ridges are broken up, three on the body of 
 the shell and the fourth under the hinge-line. 
 
 Loc. and Horizon. Near Yarrol Station, Burnett (W. H. Rands)—Gympie 
 
 Beds. 
 
 Genus—ASTARTELLA, Hall, 1858.+ 
 (Iowa Geol. Report, Pt. 2, p. 715.) 
 
 ASTARTELLA P RHOMBOIDEA, sp. nov., Pl. 14, fig. 15. 
 
 Sp. Char. Shell small, square-ovate, compressed; hinge-line much arched, very 
 oblique posteriorly ; ventral margin rounded, anterior margin more inclined to be square 
 than rounded, whilst the posterior margin is decidedly square; umbones prominent and 
 projecting ; lunule probably well marked; surface with sharp thread-like, raised, 
 equidistant, concentric striw, with more or less flat interspaces. 
 
 Obs. The more important hinge characters of this shell are at present unknown, 
 and its reference to Astartella is therefore purely suppositive. It possesses the 
 sculpture of many species, but the hinge-line is too oblique for a true Astartella. 
 
 It agrees better generally with certain forms described by the late Dr. Meek 
 from the Coal Measures of Ohio,t than it does with Hall’s type, which is amore massive 
 shell, although still small. 
 
 The sculpture of A. ? rhomboidea resembles that of Pachydomus Danai, De 
 Koninck,§ but the shell otherwise differs completely in the outline of the posterior end. 
 Again, it appears to have certain relations with the genus Scaldia, De Ryckholt, but the 
 present name will, in the meantime, serve to distinguish it. Itis certainly distinct 
 from either of the New South Wales shells referred to this genus by Prof. De Koninck. 
 
 Loc. and Horizon. Gympie (R. L. Jack)—Gympie Beds. 
 
 Genus—CYPRICARDELLA, Hall, 1858. 
 
 Cypricardella, Hall, Trans. Albany Inst., 1858, iv., Pt. 1, p. 17. 
 Microdon, Conrad (now Agassiz), Journ. Acad Nat. Sci. Philadelphia, 1842, viii., Pt. 2, p. 247. 
 
 CYPRICARDELLA JACKH, sp. nov., Pl. 14, figs. 11 and 12. 
 
 Sp. Char. Shell oblong-ovate, x oderately compressed, deeper than wide ; hinge- 
 line straight, horizontal; ventral margin very eonvexly rounded; anterior side small, 
 the margin obliquely curved; posterior margin similarly curved, but not produced ; 
 umbones anterior, small, and inconspicuous ; escutcheon well-marked and deep; lunule 
 none, the anterior border being erect and simple; surface nearly smooth, or with very 
 fine impressed concentric lines. 
 
 * King, Mon. Permian Foss. England, 1850, t. 15, f. 18-20. 
 
 + Non Astartila, Dana, 1847. 
 
 $ Ohio Geol. Report, 1875, ii., Pt. 2 (Pal.), t. 19, f. la and 0. 
 
 § Foss. Pal. Nouv,-Galles du Sud, 1877, Pt. 3, p. 278, t. 19, f. 5, 
 
277 
 
 Obs. The shell has undergone erosion about the umbones and dorsal margin, 
 which gives it arather inequivalve appearance. Its generic affinities are obscure, but it 
 resembles several forms of Cypricardella lately described by Professor De Koninck. It 
 is certainly undescribed as an Australian species. 
 
 Loc. and Horizon. Near Mount Hamilton, six miles north-east of Gympie 
 (R. L. Jack)—Gympie Beds, 
 
 Genus—ASTARTILA, Dana, 1847. 
 
 (American Journal Sci., iv., p. 155.) 
 
 ASTARTILA CYTHEREA, Dana, Pl. 14, figs. 3 and 4. 
 
 Astartila cytherea, Dana, American Journ. Sci., 1847, iv., p. 155. 
 an 55 Dana, Geology Wilkes’ U. 8. Explor. Exped., Vol. x., p. 690, Atlas, t. 4, f. 1-lg. 
 
 Sp. Char. Shell rhombic-ovate, sub-compressed. Hinge-line straight, ventral 
 margin rounded, and moderately sharp at the gape. Anterior end rather acumi- 
 nately produced, small, its margin sharply rounded; posterior end rounded, without 
 emargination, Umbones quite anterior, and much incurved and elevated; a deep 
 but not circumscribed lunule present. Surface very characteristically marked by 
 regular flattened, non-imbricating, oblique, concentric lamine, separated by shallow, 
 narrow grooves, gathering together in bundles on the anterior end, and more or less 
 striate. 
 
 Obs. The shell now under description approaches very closely, if it is not 
 identical with, Astartila cytherea, Dana, which it resembles in general outline, the 
 oblique hinge-line, and high and elevated incurved beaks. It also has a general 
 resemblance to Morris’s figure of a young individual of Pachydomus globosus,* but the 
 beaks are much smaller, and the anterior margin less defined and more excavated. It 
 is, however, an open question if the figure quoted is a Pachydomus at all. 
 
 The present shell equally resembles Pachydomus ovalis, McCoy,} and it is 
 even possible that this, and the shell referred to as figured in Dana’s work, are 
 identical. 
 
 Loc. and Horizon. Stonehumpy Creek, Bowen River (2. Hdelfelt)—Middle or 
 Marine Series, Bowen River Coal Field. 
 
 Order—CHAMACEA, 
 Family—TRIDACNID2. 
 
 Genus—EURY DESMA, Morris and Sowerby, 1845. 
 (Strzelecki’s Phys. Descrip. N. 8. Wales, &c., p. 275.) 
 
 Obs. Amongst the many interesting occurrences of New South Wales marine 
 Permo-Carboniferous fossils in Queensland, not the least is that of a Hurydesma. The 
 specimens, although calcified throughout, are much decorticated by weathering, 
 but the outline of the two valves when united, the straight posterior hinge, and the 
 deeply excavated lunular space, are all unmistakable evidences of the genus Hurydesma. 
 In the umbonal region the shells are very thick, quite an inch, and the structure of the 
 shell is very beautifully seen in some places, whilst the rugged cartilage furrows of 
 the hinge are equally apparent. 
 
 
 
 * Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, t. 10, f. 3. 
 +Ann, and Mag. Nat. Hist., 1847, xx., p. 302, t. 14, f. 4. 
 
278 
 
 EuRYDESMA corDATA, Morris. 
 
 Tsocardia ? sp., J. de C. Sby., Mitchell’s Three Expeds, Int. E. Austr., 1838, i., p. 15, t. 2 [8], f. 1 and 2. 
 Eurydesma cordata, Morris, Strzelecki’s Phys. Descrip. N.S. Wales, &c., 1845, p. 276, t. 12. 
 nf 3 Dana, Geology Wilkes’ U. S. Explor. Exped., 1849, Vol. x., p. 700. 
 
 Obs. Several large and small shells from the Yatton Gold Field may be referred 
 to this species, both from their massive shells and strong thick hinges, but they are too 
 much weather-worn for general description. Dana mentions that in the half-broken-off 
 beak of one valve “ there is a tubular cavity, filled with rock, coming up obliquely from 
 between the beaks, and passing out anteriorly, and this cavity is probably the byssiferous 
 channel.” A similar passage is visible in one of our specimens. 
 
 Loc. and Horizon. Yatton (&. L. Jack and N. H. Burrowes—Mining and Geo- 
 logical Museum, Sydney)—Gympie Beds. 
 
 EvryYDESMA saccuLus, McCoy. 
 
 Pachydomus sacculus, McCoy, Ann, and Mag. Nat. Hist., 1847, xx., p. 301, t. 14, f. 5. 
 Eurydesma sacculus, Dana, Geology Wilkes’ U. S. Explor. Exped., Vol. x., 1849, p. 700, Atlas, t. 7, f. 8a-c. 
 Obs. Several badly preserved examples are probably referable to this species. 
 One in particular shows the characteristic satchel-shaped outline, and the short posterior 
 compressed wing, The shell substance is very foliaceous, and it appears to have been 
 a much less robust shell than ZH. cordata, Morris. 
 Loc. and Horizon. Yatton (N. H. Burrowes ; Mining and Geological Museum, 
 Sydney)—Gympie Beds. 
 
 Order—VENERACEA. 
 Family—CARDITDA. 
 
 Genus—CONOCARDIUWNM, Bronn, 1835. 
 (Lethzea Geognostica, 1, p. 91). 
 
 CONOCARDIUM AUSTRALE, WcCoy, Pl. 14, fig. 6. 
 
 Pleuororhynchus australis, McCoy, Ann. and Mag. Nat. Hist., 1847, xx., p. 30, t. 16, f. 4. - 
 Conocardium australe, Etheridge fil., Cat. Australian Foss., 1878, p. 68 (for synonymy.) 
 
 Obs. The Gympie Beds have yielded a single example of a Conocardiwm, larger than 
 Prof. McCoy’s figure, but resembling his species in outline and appearance, except that 
 the two diverging impressed lines on the shorter end of the shell are not visible. The 
 difference in the strength of the striz on the portions which would be bounded by these 
 impressed lines is, however, quite apparent, and as described by McCoy. ‘The carina of 
 C. australe has a peculiar curve characteristic of the species. 
 
 Loc. and Horizon. Gympie (R. L. Jack)—Gympie Beds. 
 
 Order—MYACEA. 
 Family—ANATINIDA. 
 
 Genus—CHANOUYA, F. B. Meek, 1866. 
 (Ral. Up. Missouri, Pt. i., p. 42.)* 
 
 Obs. The following species are provisionally referred to this genus, pending a 
 detailed examination of allied forms from the Marine Series of the New South Wales 
 Permo-Carboniferous rocks. It has been pointed out by Dr. Paul Fischer,t that the 
 
 * Smithsonian Contributions to Knowledge, 1866, Vol. xiv., No. 172. 
 + Man, Conchyl. et de Pal, Conchyl., 1877, p. 1167. 
 
279 
 
 European species referred by the late Prof. De Koninck to this genus do not wholly 
 accord with those for which it was originally proposed by the late Dr. Meek. It is 
 possible that the same objections can be raised against the Australian shells.* 
 
 Cumyomya ? Erueriparr, De Koninck, sp. 
 Sanguinolites Etheridgeit, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 262, t. 17, f 2 
 (non t. 16, f. 2). 
 
 Sp. Char. Shell of medium size, gibbous, curved, more or less oblique, and pro- 
 duced posteriorly ; flanks very gibbous in the visceral region, rapidly decreasing to 
 the ventral margin. Cardinal margin or hinge-line less than the length of the shell, to 
 some extent curved upwards; ventral margin somewhat obliquely curved from before 
 backwards. Anterior end subtruncate ; posterior end obliquely and abruptly truncate, 
 with a narrow gape. Umbones anterior and prominent; diagonal ridge rounded ; 
 posterior slope flattened. Lunule apparently elongated and narrow; escutcheon 
 wide, and moderately long. Lines of growth rugged and coarse, with intermediate 
 finer striz. 
 
 Obs. The specimen from which the above characters are taken is rather 
 crushed, and they are therefore open to modification. The diagonal groove represented 
 in De Koninck’s figure is not visible in the present example. It isa much longer species 
 than Chenomya ? acuta, Etheridge, and the dorsal margin appears to rise rather more. 
 In specimens of ©, Htheridget from the Maitland Coal Measures the diagonal ridge varies 
 much in its development ; in some it is very pronounced, in others but little apparent. 
 How much of this is due to pressure and distortion it is difficult to say, but in some 
 specimens it undoubtedly is the case, as it is accompanied by a greater or less degree 
 of artificial inequivalvism; but in all such cases the width of the valves is much 
 increased, as if by pressure from above. 
 
 Loc. and Horizon. Banana Creek, near Banana, Dawson River (H. Mackay ; 
 Colln. De Vis)—Middle or Marine Series, Bowen River Coal Field; ? Gympie (W. H. 
 Rands)—Gympie Beds. 
 
 CHENOMYA ? CARINATA, sp. nov., Pl. 43, figs. 5 and 6. 
 
 Sp. Char. Shell rhomboidal, short, oblique, gibbous, produced posteriorly, 
 highly carinate. Cardinal margin short ; lunule short and wide; escutcheon moderately 
 wide and shallow, with sharp margins; ventral margin obliquely rounded. Anterior 
 end small, very oblique ; posterior end obliquely truncate, slightly gaping. Diagonal 
 ridge very marked, prominent, and sharp ; posterior slope concave, with a median groove 
 or depression. Umbones prominent and terminal, incurved. Concentric ridges very 
 coarse and widely separated, ending at the diagonal ridge, or but very little marked on 
 the posterior slope. 
 
 Obs. These characters are taken from a decorticated specimen. This isa very 
 marked shell when viewed in profile, from the great prominence of the diagonal ridge. 
 When seen from above, across the valves, its great width at once attracts notice, being 
 quite two-thirds the length of the shell. The short form, and the wide, highly 
 carinate condition, without any sign of distortion, lead me to regard this as a distinct 
 species. 
 
 Loc. and Horizon. Banana Creek, near Banana, Dawson River (H. Mackay ; 
 Colln. De Vis)—Middle or Marine Series, Bowen River Coal Field. 
 
 * They certainly are not Sanguinolites, as that genus was restricted by De Koninck (see p, 281). I 
 hope to work the groups out shortly. (2.E. Junr.) 
 
280 
 
 CHz#NoMYA? acuta, Etheridge, sp. 
 Panopeaplicata, var. acuta, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 342, t. 21, f. 3 and 3a. 
 
 Obs. My Colleague states that the shell referred by Mr. Etheridge to the 
 Cretaceous species Panopea plicata, Sby., under the varietal name acuta comes from the 
 Permo-Carboniferous Series of the Bowen River Coal Field, and can therefore bear no 
 relation to the form described by Sowerby. 
 
 Mr. Etheridge remarks that “our shell is more acute than Sowerby’s typical 
 form, the posterior or anal border or extremity in this variety being less truncated ; it, 
 however, gapes as much.”’ It is not impossible that this fossil may be a species of 
 Chenomya, although we at present know little of the external sculpture, whether granu- 
 lar or not. It is even possible, judging from the difference in outline of Mr. Etheridge’s 
 figures, that two species have been placed under the one name. 
 
 Loc. and Horizon. Pelican Creek, Bowen River (The late R. Daintree)—Middle 
 or Marine Series, Bowen River Coal Field. 
 
 CHENOMYA? BOWENENSIS, sp. nov. 
 Sanguinolites (comp. S, clava, McCoy), Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 302, t. 16, f. 54, 
 
 Sp. Char. Shell transversely elongate, produced, nasute, and sharp posteriorly, 
 closed, very convex in the visceral region, rapidly decreasing towards the ventral margin. 
 Cardinal margin or hinge-line straight; ventral margin convex; anterior end gibbous 
 and inflated; posterior end much compressed or flattened, wedge-like, attenuating 
 rapidly to a sharp, thin margin, which is narrowly rounded. Umbones quite anterior 
 and terminal, inrolled, and depressed from above ; no diagonal ridge, or defined posterior 
 slope, but the flanks of the valves much inflated and gibbous. Lunule apparently some- 
 what cordate. Surface with rather broad, concentric lamelle of growth, forming 
 coarse ruge on the flattened posterior end. 
 
 Obs. I formerly regarded this shell as a Sanguinolites and compared it to S. clava, 
 McCoy, but it cannot be placed in that genus as now restricted. The following remarks 
 were then made :—‘‘ With the exception of a somewhat shorter and more gibbous form, 
 I am unable to distinguish this species from Prof. MeCoy’s S. clava. The specimen is 
 a decorticated cast, there are no traces of muscular impressions left, and the valves have, 
 by pressure, been slightly displaced. Notwithstanding this it is easily seen that the 
 shell possessed a much more gibbous and rotund habit than 8. clava, the relative 
 convexity of the valves immediately below the beaks being greater. The rapid attenua- 
 tion of the flanks towards the ventral margin, and the thinning-off of the posterior end, 
 are as in S. clava, and there also existed a well-marked lunette and escutcheon, although 
 the latter was much shorter than in McCoy’s species. Lastly, the posterior slope is 
 more defined in the Australian form, and the valves were closed posteriorly. Taking 
 all these characters together, it must be conceded that, in all probability, the two species 
 are distinct. A useful comparison might be made between Mr. Jack’s shell and two 
 Australian species described by Dana, did we only know more about them, viz.:— 
 Edmondia? (Pholadomya) glendonensis,* and Sanguinolites or Edmondia? (Phola- 
 domya) undata.t The first, as figured by Dana, is a crushed-down shell, without form 
 or character, and is simply unrecognizable; all one can say is, that it appears to be a 
 shorter form than that now under discussion. The second is a very Sanguinolites-like 
 shell, and is clearly separated from the latter by the position of the beaks, more than 
 sub-central in position, and the consequently larger anterior end. 
 
 
 
 * Geology Wilkes’ U. 8. Explor. Exped., 1849, Vol. x., Atlas, t. 2, f. 12. 
 + Loe, ctt., f, 11. 
 
 
 
281 
 
 A glance at the so-called species of Sanguinolites described * from the Carboni- 
 ferous beds of New South Wales by Professor De Koninck (8. Etheridgei, S. Mitchellit, 
 S. MeCoyt, and 8. Tenison?), will show how little resemblance they bear to the Queensland 
 fossil. Of them, 8. WeOoyi is certainly more nearly allied to the latter than any of the 
 others. It has the outward appearances of the genus Allorisma, King,t but without a 
 better knowledge of its internal characters it would not be wise to so refer it. It is 
 certainly clear that, like the latter, it possessed an external ligament, but the impression 
 of the pallial line is not retained. Again, the valves are more convex than is usually 
 seen in Allorisma. 
 
 Loc. and Horizon. Coral Creek, Bowen River, below Sonoma Road-crossing 
 (R. L. Jack)—Middle or Marine Series, Bowen River Coal Field. 
 
 Genus—EDMONDIA, De Koninck, 1842. 
 (Descrip. Anim. Foss, Terr. Carb. Belgique, p. 66,) 
 
 Epmonpra ? opovata, HLtheridge. 
 Edmondia obovata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 328, t. 18, f. 3. 
 
 Sp. Char. ‘Shell ovate, anterior margin convex, or nearly circular; posterior 
 margin slightly truncated; hinge-line nearly straight; umbones small, close to anterior 
 side ; ventral margin almost parallel with dorsal; outer shell wanting, but appears to 
 have been concentrically banded.” (£theridge.) 
 
 Obs. This species was compared by Mr. Etheridge to Pullastra ovalis, McCoy, 
 and Hdmondia ? compressa of the Irish Carboniferous System. 
 
 It is an extremely difficult matter appropriating these indistinct casts to their 
 proper genera. The present specimen is certainly not a MMyacites, as alternatively 
 suggested by its describer, nor does it agree well even with the characters of Hdmondia. 
 The figure seems to me to agree much more with the outline of the last genus, 
 Chenomya ?, than it does with either of the foregoing. 
 
 Loc. and Horizon. Beehive Reef, Gympie (Zhe late R. Daintree) —Gympie 
 Beds. 
 
 Genus—SANGUINOLITES, McCoy, 1844.t 
 (Synop, Carb. Lime. Foss. Ireland, p. 47 ; Brit. Pal. Foss., 1852, Fasc. 2, p. 276.) 
 
 SANGUINOLITES ConcENTRICUS, Etheridge, sp., Pl. 43, fig. 7. 
 Edmondia concentrica, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 328, t. 13, f. 2. 
 
 Sp. Char. Transversely elongated, oblong, valves rather compressed, hollowed 
 on the flanks. Cardinal or dorsal margin straight posteriorly, inclined obliquely at the 
 anterior end; ventral margin convex anteriorly and posteriorly, straight medianally. 
 Anterior end long, narrowed, and flattened ; posterior end longer than the anterior, with 
 a semi-truncate margin; posterior slope very much flattened, hardly defined by any 
 diagonal ridge, and entire. Umbones inconspicuous, depressed, sub-median in position. 
 Surface with numerous concentric lines of growth, arranged in band-like zones, distant 
 from one another. 
 
 * Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, pp. 261-265, t.16and17. These are not Sanguinolites, 
 as the genus is now restricted. 
 
 + Mon. Perm. Foss. England, 1850, p. 196. 
 
 + Restricted, De Koninck, Faune Calc. Carb. Belgique, 
 
282 
 
 Obs. A very poor example was figured by Mr. Etheridge to “draw the atten- 
 tion of Australian geologists to the Lamellibranchiata of the Paleozoic rocks of 
 Queensland, and elsewhere through the colony, in the hope that search may be made 
 for more perfect specimens.” 
 
 As the anterior of the shell is unknown its generic affinity must remain doubtful, 
 but it seems to accord better with the late Prof. De Koninck’s restriction of 
 Sanguinolites than with Edmondia, to the type species of which it bears resemblance. 
 There is a decided posterior slope present, but only the faintest trace of a diagonal 
 ridge. 
 
 Loc. and Horizon. Gympie (The late R. Daintree—G. Sweet); the Gas Works, 
 Gympie (W. H. Rands)—Gympie Beds. 
 
 Family—SAXICAVID. ? 
 
 Genus—PACH YDOMUS, Morris, 1845. 
 (Strzelecki’s Phys. Descrip. N. S. Wales, &c., p. 271.) 
 
 Obs. In the “ Catalogue of Australian Fossils,” and in the description of the 
 “ Fossils of the Bowen River Coal Field,” attention was called by the Writer to the 
 difficulties attending a proper distribution of the species of Dana’s genera, M@onia (vel. 
 Myonia), Pyramia (vel. Pyramus), and Cleobis as pointed out by the late Dr. Stolitzka. 
 In Professor Dana’s first Paper on Australian Paleontology, contributed to the pages of 
 the American Journal of Science, the three were described as separate and distinct 
 genera, but in the more extended account of the Geology of the “Wilkes Exploring 
 Expedition” they were united under the one name Meonia. Dana at the same time 
 stated that his Pyramia was identical with Notomya, McCoy. The arrangement adopted 
 in the Catalogue was a purely provisional one, proposed more as a temporary suggestion 
 than as an accurate solution of a difficult and obscure subject. Reasons were also given 
 for adopting the name Notomya, McCoy, in preference to any of the others. 
 
 Further study of this subject has not ended in any very satisfactory result, as the 
 material in the National Collection, London,* although large, is not sufficient for the 
 purpose in view. Added to this, the discrepancies between the various descriptions are 
 so marked that it becomes quite impossible to adjudicate on the relations of the species 
 referred to the genera in question. Pachydomus and Notomya will probably stand as 
 good genera, certainly the former, and it is quite possible that it will be necessary to 
 some extent to rehabilitate Weonia, Dana. 
 
 I hope, before any lengthened period has passed away, to make a complete study 
 of this group of shells, but from the paucity of material 1t will be no easy task. 
 
 Pacnybomus eLozosus, J. de C. Sowerby, sp. 
 
 Megadesmus globosus, J. de C. Sowerby, Mitchell’s Three Expeds. Int. E. Australia, 1888, i., p. 15, t. 3, 
 ff. 1 and 2. 
 Pachydomus globosus, Morris, Strzelecki’s Phys. Descrip. N. 8S. Wales, &c., 1845, p. 272, t. 10, f, 2 and 3. 
 Cleobis grandis, Dana, American Journ. Sci., 1847, iv., p. 154. 
 Meeonia grandis, Dana, Geology Wilkes’ U. 8S. Explor. Exped., Vol. x., 1849, p. 697, t. 6, f. 8. 
 Pachydomus globusus (pars.), Etheridge fil., Cat. Australian Foss,, 1878, p. 75. 
 cs > Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 301. 
 
 Obs. The fossiliferous rock of Pelican Creek has furnished a ponderous example 
 of this species, but in a wretched state of preservation, without any trace of shelly 
 matter remaining, and the whole substance of the cast having assumed the form of a 
 
 
 
 * This was written before I had left London. Iam sorry to say that I do not find that the material 
 in Sydney will advance the subject much. (RZ. Jun. 
 
 
 
 
 
283 
 
 decomposed ferruginous ironstone nodule. The specimen measures roughly about eight 
 inches by five and a half, without the shelly matter. Across the dorsal region, from the 
 one rounded diagonal ridge to the other, the shell measures at least five inches. This 
 will give some idea of the great breadth attained by this species, and its general globose 
 or gibbous outline. The umbones are very large, incurved, and quite anterior. Judging 
 by the space occupied by matrix between the cardinal edges of the two valves, the 
 ligament must have been of great dimensions and strength. The collection contains 
 two examples of this species, that from which the foregoing notes are taken, and a 
 smaller one, which is believed to represent the young condition of the species. The 
 latter, when held in certain lights, shows indistinct traces of radiating strie in the cast. 
 Upon examining a remarkably fine specimen in the late Count Strzelecki’s Collec- 
 tion, I find that it also, where the shelly matter is worn off, exhibits similar radiating 
 ridges. In the paper on the Bowen River Coal Field Fossils I overlooked the fact that 
 Prof. J. D. Dana had already ealled attention* to the identity of his Cleobis grandis and 
 Pachydomus globosus, Morris. 
 
 My Colleague has obtained a specimen, denuded of all external shelly matter, 
 from the Gympie Gold Field, which, although small, may be an individual of the 
 present species ; it is, however, too imperfect to name definitely. 
 
 Loc. and Horizon. . Pelican Creek, Bowen River, half-a-mile above Sonoma Road- 
 crossing, in a highly fossiliferous concretionary and ferruginous mudstone; Pelican 
 Creek, in a sandstone above the Garrick Coal-seam—both horizons in the Middle or Marine 
 Series, Bowen River Coal Field (2. LZ. Jack). 
 
 Genus—MAONTA, Dana, 1847. 
 
 Myonia, Dana, American Journ. Sci., 1847, iv., p. 158, 
 Meonia, Dana, Geology Wilkes’ U. 8. Explor, Exped., Vol. x., 1849, p. 694. 
 
 Obs. This genus is provisionally used, pending a detailed examination of all 
 these dubious Permo-Carboniferous Bivalves, for shells after the type of I. elongata, 
 Dana, and I. carinata, Morris, sp. The muscular system of the latter is quite different 
 to that of various genera in which it has been placed, and accords better, although not 
 exactly, with the characters of I/@onia as laid down by Dana in his latter description. 
 
 Mamonta cartnata, Morris, sp. 
 
 Pachydomus carinatus, Morris, Strzelecki’s Phys. Descrip. N. 8. Wales, 1845, p. 278, t. 11, f. 3 and 4. 
 Cypricardia rugulosa, Dana, American Journ, Sci., 1847, iv., p. 157. 
 Pachydomus carinatus, McCoy, Ann. and Mag. Nat. Hist., 1847, xx., p. 301. 
 Meconia ? carinata, Dana, Geology Wilkes’ U. 8S. Explor. Exped., p. 696, Atlas, t. 6, f. lw and b. 
 Pleurophorus ? carinatus, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 283, t. 19, f. 8. 
 Pachydomus ? carinatus, Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 300, t. 16, f. 53. 
 Notomya (Mconia) elongata, Ratte (non Dana), Proc. Linn, Soc. N. 8. Wales, 1887, ii., Pt. 1, p. 189, t. 3. 
 
 Obs. The strongly marked umbonal ridge, and the slightly concave posterior 
 slope, at once mark this species as peculiar. Two specimens in a moderately good state 
 of preservation were obtained in the Bowen River Coal Field; both have the entire 
 shell removed, and are therefore in the form of casts, but with the exception of some 
 slight displacement of the valves, the general outline is retained. I formerly placed 
 this species in Pachydomus, but both this reference and Prof. De Koninck’s to the 
 genus Plewrophorus I now believe to be erroneous. ‘The shell does not coincide with the 
 original types of Pachydomus, such as P. antiquatus and P. cuneatus.¢ With regard to 
 
 * American Journ. Sci., 1848, v., p. 435. 
 + Megadesmus, J. de C. Sowerby, in Mitchell’s Three Expeds. Int. E. Australia, 1838, i,, p, 15, t. 1, 
 f° 2 and 3. 
 
284 
 
 Pleurophorus, I have quite failed to trace a dental structure in any of the casts of 
 M. carinata examined, and of which there are several good examples in the Australian 
 Museum. J. carinata seems to be wholly devoid of hinge teeth, but possesses a very 
 peculiar system of muscular scars. These have been well figured by the late Mr. Felix 
 Ratte,* and still further show its dissimilarity to Pleurophorus. 
 
 The double anterior and fringed muscular scars, and the accessory scars at the 
 apex of the beaks, accord with the characters originally laid down by Dana for his 
 genus Meonia, and i think it not improbable that this name will have to be retained for 
 transversely elongate shells with the above characters, typified by JZ elongata, Dana, 
 and Pachydomus carinatus, Morris. 
 
 Loe. and Horizon. Coral Creek, Bowen River, below Sonoma Road-crossing ; 
 Bowen River, at No. 25 Traverse Station (&. LZ. Jack)—Middle or Marine Series, 
 Bowen River Coal Field. 
 
 Monta recta, Dana. 
 
 Cleobis recta, Dana, American Journ, Sci., 1847, iv., p. 154. 
 Meonia recta, Dana, Geology Wilkes’ U. S. Explor. Exped., 1849, Vol. x., p. 698, ‘Atlas t. (pain e4 
 Notomya (Mconia) recta, Etheridge fil., Proc. R. Phys. Sec. Edinb., 1880, v., p. 299. 
 
 Obs. The chief characters of this species are its very inequilateral and oblong 
 form with the parallel dorsal and ventral margins. Professor Dana’s specimen 
 measured three and a-half inches in length, but the shell here referred to C. recta 
 measures seven and a-quarter inches in the same direction. Like all the Bivalves in 
 my Colleague’s Bowen River Collection, the state of preservation is very bad, but there 
 appears to be the remains of an obscure posterior slope, a character which is not 
 mentioned in Dana’s description. 
 
 The generic affinities are by no means clear, a state of matters common to a 
 number of these Bivalves, and even Dana appears to have figured an imperfect example. 
 
 Loc. and Horizon. Coral Creek, Bowen River, below Sonoma Road-crossing, in 
 a yellow micaceous decomposed ironstone, of the Middle or Marine Series, Bowen 
 River Coal Field (&. LZ. Jack). 
 
 Class—GASTEROPODA. 
 
 Order—PROSOBRANCHIATA. 
 Family—NATICID. 
 
 Genus—NATICOPSIS, McCoy, 1844. 
 (Synop. Carb. Lime. Foss. Ireland, p. 33.) 
 NatIcoPsis ? HARPHFORMIS, Ltheridge, Pl. 15, fig. 10. 
 Naticopsis harpeformis, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 337, t. 18, f. 6. 
 
 Obs. Under the above name Mr. Etheridge figured a fragment of a very 
 problematical fossil. He considered it to be a portion of the body-whorl of a naticiform 
 shell, the suture being ornamented with ‘thirty or thirty-five nodes or tubercules, each 
 of which occupies the summit of a rib or varice.” He further pointed out that the 
 whorls of some species of Loxonema are similarly ornamented. On the other hand, 
 Prof. John Morris suggested that the fossil might be a portion of a small Goniatites, 
 with a wide umbilical cavity. 
 
 Either of these views may be the correct one, so very doubtful are its affinities. 
 
 Loc. and Horizon. Don River (Lhe late R. Daintree)—Gympie Beds. 
 
 * Proc. Linn, Soc, N. S. Wales, 1887, ii., Pt. 1, p, 139, t. 3. 
 
 
 
 
 
 
 
285 
 
 Naticopsts vARTATA, Phillips, sp.? 
 
 Natica variata, Phillips, Tl, Geol. Yorksh., 1836, Pt. 2, p. 224, t. 14, f. 26 and 27. 
 Naticopsis variata, McCoy, Brit. Pal. Foss., 1852, fas. 2, p, 544. 
 
 Obs. We are acquainted with a shell possessing the general outline of this 
 species, but only in the form of casts, from the Corner Creek Beds. The spire was 
 small, the body-whorl large and ample, and the ornament consisted of strong stria 
 in and emerging from the suture, as in the above species. On the other hand, the spire, 
 although small, was, perhaps, rather too large for WV. variata, and it has therefore been 
 thought advisable to give this determination with a note of interrogation. 
 
 Loe. and Horizon. Corner Creek, Great Star River (Rk. L. Jack)—Star Beds. 
 
 Naticopsis, sp. ind. 
 [Compare WV. elongata, Phill., loc. cit., t. 14, f. 28.] 
 
 Obs. <A single cast obtained from the same beds by Mr. P. W. Pears resembles 
 Naticopsis elongata, Phill., in obliquity and general appearance, although a subangula- 
 tion of the body-whorl will probably separate the two forms. It likewise has rather 
 the appearance of some Platyostome, but is devoid of the reflected and sinuous lips of 
 those shells. It is difficult to say how far distortion might alter the outline of the 
 shells previously compared to Naticopsis variata, but hardly to such an extent as to 
 merge the two forms under consideration into one. 
 
 Loc. and Horizon. Corner Creek, Great Star River (P. W. Pears)—Star Beds. 
 
 Family—PYRAMIDELLID 2. 
 
 Genus—LOXONEMA, Phillips, 1841. 
 (Pal. Foss. Devon., p. 98.) 
 
 Obs. A crushed example of a Loxonema (Pl. 15, fig. 17), of a type common in 
 Carboniferous rocks was communicated by the late Mr. James Smith. The whorls are 
 ribbed with many longitudinal, slightly bent ridges or coste. There are traces of ten 
 faintly convex whorls. The shell is of the type of Loxonema rugifera, Phill. 
 
 Loe. and Horizon. Stony Creek, Stanwell, near Rockhampton (The late 
 J. Smith)—Gympie Beds. 
 
 Family—EUOMPHALID. 
 
 Genus—BUOMPHALUS, J. Sowerby, 1814.* 
 (Min. Con., p. 97.) 
 
 Obs. The presence of this genus in the Permo-Carboniferous of Queensland is 
 placed beyond doubt by the occurrence of a few indifferently preserved casts in the 
 Stanwell Beds. None are sufficiently well preserved for specific description, but two 
 undoubtedly indicate the genus as now restricted and typified by Huomphalus pentangu- 
 latus. The best of these has a diameter of one inch, the under surface round, and the 
 upper supporting a sharp prominent keel ; in fact the whole appearance of the shell is 
 very much that of the species named. 
 
 In the Star River Beds a number of small Euomphaloid shells (Pl. 14, fig. 21) 
 are met with. The test has entirely disappeared, and the specimens have undergone so 
 much decay that it is with difficulty they can be assigned to any particular genus. 
 Their place will probably be found with the present one. 
 
 Loc. and Horizon. Stony Creek, Stanwell, near Rockhampton (The late James 
 Smith)—Gympie Beds. 
 
 * Emended, De Koninck, Faune Cale. Carb. Belgique, Pt. 3 (Ann. Mus. R. Hist. Nat. Belgique, 
 1881, vi.), p. 156. 
 
286 
 
 Genus—PLATYSCHISMA, McCoy, 1844. 
 (Synop. Carb. Lime. Foss. Ireland, p. 38.) 
 
 PLATYSCHISMA ocuLUS, J. de C. Sowerby, Pl. 15, figs. 3 and 4. 
 
 Trochus oculus, J. de C. Sowerby, Mitchell’s Three Exped. Int. E. Australia, 1838, i., p. 15, t. 2, 
 f. 3.and 4. 
 
 Platyschisma oculus, Morris, Strzelecki’s Phys. Descrip. N. S. Wales, 1845, p. 286, t. 18, f. 1. 
 
 Euomphalus oculus, De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 330, t. 23, f. 18. 
 
 Obs. Two specimens, which I am quite unable to refer to any other than this 
 species, have been obtained through the painstaking efforts of the late Mr. James 
 Smith. Neither is in a good state of preservation, one being only a portion of a 
 specimen, whilst the other was evidently much crushed during the life of the shell, and 
 naturally repaired, whereby the base has been obliquely pressed inwards, and the 
 umbilicus thrown out of place. The body-whorl is, to some extent, channelled or 
 flattened along the suture, afeature also visible in some varieties of P. oculus. 
 
 Loc. and Horizon. Stony Creek, Stanwell, near Rockhampton (The late James 
 Sinith)—Gympie Beds. 
 
 PLATYSCHISMA RoTUNDA, Etheridge, Pl. 15, fig. 6. 
 Pleurotomaria rotunda, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 336, t. 18, f. 3. 
 
 Sp. Char. Shell turbinate or trochiform, with four whorls; apex slightly 
 depressed ; aperture suboval or subangular. Whorls completely rounded and concentri- 
 cally striated, with numerous close-set costs, which are crossed diagonally from the 
 mouth backwards by very fine lines, giving the shell a reticulate appearance. Base 
 slightly convex. Umbilicus very small or obsolete. Sinus scarcely distinguishable. 
 (Etheridge.) 
 
 Obs. This shell appears at first sight to be smooth, the ornamentation being 
 microscopic, yet definite; on a portion only of the shell is there structure remain- 
 ing. In form, size, and general aspect, P. rotunda resembles P. granulata, De 
 Kon., but the sculpturing of the shell, and the band-like sinus, remove it from 
 that species. P. votundata, Phill., in the rotundity of the whorls and other 
 minor points, somewhat resembles it, but our species is much less acute in the spire. 
 (Ltheridge.) 
 
 Platychisma rotunda possesses a most suspicious resemblance to P. oculus, but 
 the figure of the former affords no evidence of an umbilicus, and its umbilicus is even 
 described as very “small or obsolete.” If there is no umbilicus, or, on the other hand, 
 if the shell really has a band and sinus, it cannot be a Platyschisma, but generally it very 
 closely resembles this genus. 
 
 An impression of a much smaller shell, but one otherwise resembling P. rotunda, 
 has been collected by Mr. C. W. De Vis in the Rockhampton Beds. The spiral strize 
 mentioned in the above description are not visible, but the diagonal lines are very 
 apparent, and are more or less sigmoidal. On the whole it very much resembles a young 
 condition of Platyschisma rotunda. 
 
 Loc. and Horizon. Cracow Creek, Dawson River, Lat. 25° 20’ S., Long. 150° 
 15’ E., approximately (The late R. Daintree)—Middle or Marine Series, Bowen River 
 ©oal Field; Rockhampton District* (C. W. De Vis; Colln. De Vis)—Gympie 
 Beds. 
 
 
 
 * See note, p. 199, 
 
 
 
 
 
287 
 
 Family—PLEUROTOMARITD 2. 
 
 Genus—PLEUROTOMARIA, Defrance, 1824. 
 (Tableau, p. 114.) 
 
 PLEUROTOMARIA CARINATA, J. de C. Sby.?, Pl. 15, fig. 16. 
 ? Pleurotomaria carinata, J. de C. Sowerby, Min. Con., vii., p. 70, t. 640, f. 3. 
 Pleurotomaria carinata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 331, t. 15, f. 6. 
 
 Sp. Char. Shell depressed, composed of three or four whorls; base flat ; body- 
 whorl large, expanded, the two upper whorls (in our specimen) distorted ; umbilicus not 
 seen; shape of aperture doubtful ; no shell structure left. (Htheridge ) 
 
 Obs. I can scarcely detect any difference between the form and habit of this 
 shell and those of Plewrotomaria carinata, Sby. Its size is greater ; but unfortunately 
 the loss of the outer shell prevents our seeing the band or slit at the edge of the whorl, 
 in the absence of which it might be referred to Raphistoma or Platyschisma ; it is not, 
 however, sufficiently depressed to be referred to the former genus. (EHtheridge.) 
 
 If this shell is correctly referred to J. de C. Sowerby’s Pleurotomaria, it must be 
 very much distorted, for the species in question does not possess the obliquity of the 
 Queensland shell, nor is the band on the body-whorl so sharp and prominent. From 
 the condition of the specimen, as represented by the figure, it is impossible to say 
 to which section of the large genus Plewrotomaria—whether Ptychomphalus, Agassiz, 
 or Mourlonia, De Koninck—it should be referred. 
 
 Loc. and Horizon. Gympie (Lhe late R Daintree)—Gympie Beds. 
 
 Genus—MOURLONIA, De Koninck, 1883. 
 (Ann. Mus. R. Hist. Nat. Belgique, viii., p. 75.) 
 
 Movrtonta Strzeveckiana, Morris, sp., Pl. 15, fig. 2. 
 
 Plewrotomaria Strzeleckiana, Morris, Strzelecki’s Phys. Descrip. N. 8. Wales, &c., 1845, p. 287, t. 18, f. 5. 
 % =p Plews, Min. Inst. Journ., 1858, vi., Pt. 3, t. 4, fig. 
 
 Obs. To this species is referred an internal cast, with the whole of the test 
 removed. It is about two inches in height, with four whorls remaining, but on the 
 whole it appears to be a rather more inflated form than the type figured by the late 
 Professor Morris. The band is but very faintly preserved on the fore part of the 
 body-whorl. 
 
 The specimen is much too high a shell for Platyschisma rotunda, Etheridge, 
 although generally like it. The whorls are rounder, and there is an entire absence of 
 angulation. 
 
 An internal cast of four or more whorls of a roundly whorled shell, without 
 any distinctive character, or angulation of the spiral, but possessing a. distinct and well- 
 marked band, has been collected in the Burnett District, and may be the present species. 
 There is a moderately large umbilicus. 
 
 Loc. and Horizon. © Blenavon, near Rockhampton (The late James Smith) ; 
 Sandstone, near Yarrol Station, Burnett (W. H. Rands)—Gympie Beds. 
 
 Movrtonta ? CONIFORMIS, sp. nov., Pl. 41, fig. 5. 
 
 Sp. Char. Shell elongately conical, six to seven whorls, each somewhat convex 
 above the band, which is sutural and straight-sided; body-whorl, mouth, &c., not pre- 
 served. Ornament consists of strong spiral cost, distinct from one another, crossed 
 by oblique and finer lines, giving rise to a coarse reticulation. 
 
288 
 
 Obs. This unsatisfactory specimen is figured more as a record of a species than 
 as affording detailed characters of the same. The specimens are impressions of the 
 apical portions from which casts have been taken. The reference to Mourlonia is even 
 provisional, and has been made from the outward resemblance of the fossils to species of 
 that genus. 
 
 Loe. and Horizon. Banana Creek, near Banana, Dawson River (H. Mackay ; 
 Colln. De Vis)—Middle or Marine Series, Bowen River Coal Field. 
 
 Genus—YVANIA, Bayle, 1885.* 
 
 Obs. YVvania is another offshoot from the old genus Pleurotomaria, in its 
 Carboniferous sense. It is, in fact, a turriculated Pleurotomaria, in which the 
 horizontal and vertical portions of each whorl unite ina right angle. The band and its 
 sinus are on the flat or horizontal portions, and it is impossible to see them in a side or 
 profile view. The shells are ornamented by spiral grooves and ridges, and there is a 
 small umbilical fossette. 
 
 Yvania is typified by the Belgian Trochus Yvanii, Leveillé. 
 
 Yvanta Kontnext, Hth. jil., Pl. 41, fig. 7. 
 Baylea Koninckii, Eth. fil., Records Geol. Survey N. 8. Wales, 1890, i., Pt. 2, p, 82. 
 
 Sp. Char. Shell small, conical, of about six angular and deeply carinated whorls. 
 Aperture unknown. Upper portion of the whorls not absolutely flat, but a little 
 sloping, at the edge of which, and the vertical part of the whorl, is situated the band. 
 On the former are placed eight sharp, spiral ridges, with wide semi-concave interspaces, 
 but no evidence of any cross striation. Umbilicus small and inconspicuous. Height, 
 eight millimetres (in a broken state). 
 
 Obs. This is a very pretty shell, coming nearest to the European Yvania 
 spirata, De Koninck; it is, however, much less in size and has a more prominent 
 band. 
 
 Loe. and Horizon. Rockhampton District + (C. W. De Vis ; Colln. De Vis)— 
 Gympie Beds. 
 
 Genus—LUOIELLA, De Koninck, 18838. 
 (Ann. Mus. R. Hist Nat. Belgique, viii., p. 107.) + 
 
 Obs. A depressed, conical, and trochitorm Pleurotomaria-like shell, usually 
 rough and lamellar, and variously ornamented. The body-whorl frequently becomes 
 flattened and partially horizontal, with a sharp periphery, below which, on the lower 
 side, the band is situated. 
 
 Casts of a small shell have been found in the Rockhampton Beds, probably 
 referable to this genus. 
 
 Lucretia? Grayva, sp. nov., Pl. 41, fig. 6. 
 
 Sp. Char. Depressed trochiform, of four or five whorls, the upper ones conical, 
 but the body-whorl more or less concave, turning upwards towards the periphery, 
 which is sharp. Surface of each whorl crossed by transverse oblique and curved 
 strie, and with equally fine spiral striz, the points of intersection becoming minutely 
 nodular, producing a most delicate reticulation. 
 
 * Teste Fischer (Man. Conchyl. et de Pal. Conchyl., 1887, p. 857) = Baylea, De Koninck (Ann. Mus, 
 R. Hist. Nat. Belgique, 1883, viii., p. 68), non Bayleita, M. Chalmas, 1873. 
 
 + See note, p. 199. 
 
 t Faune du Calcaire Carbonifére de la Belgique, Pt. 4. 
 
 
 
289 
 
 Obs. The under surface of this interesting shell is unknown, and it is with 
 some doubt that the reference to Lwciella is made; on the other hand, I do not know 
 in what other genus to place it. Unfortunately, like so many of the Queensland 
 fossils, the specimens are but impressions, and indifferent ones. 
 
 I have much pleasure in naming the species after Mrs. Robert Gray, of 
 Edinburgh, an ardent Collector, and to whom Prof. Alleyne Nicholson and the Writer 
 were indebted, in years gone by, for an opportunity of describing many interesting 
 fossils. 
 
 Loc. and Horizon. Rockhampton District * (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 Genus—MURCHISONTIA, D Archiac and De Verneuil, 1841. 
 (Bull. Soc. Géol. France, xii., p. 154.) 
 
 Muvrcnisonta CaRrinata, HLtheridge, Pl. 15, fig. 9. 
 Murchisonia carinata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 337, t. 18, f. 5. 
 
 Sp. Char. Shell elongated, of many whorls (four exposed), strongly keeled or 
 earinated along the middle of each whorl; no ornamentation seen, being a cast only. 
 (Etheridge.) 
 
 Obs. Although but a very simple form of Murchisonia, Mr. Etheridge was 
 unable to name any species with which it corresponded. The position of the angulation 
 of the whorl, low down, and presumedly also that of the band, with the proportions of 
 the whorls, should serve to distinguish the species. 
 
 Loe. and Horizon. Don River (The late R. Daintree)—Gympie Beds. 
 
 Other fragmentary remains of this genus have been obtained by Mr. C. W. De Vis 
 in the Rockhampton Beds, but they are quite beyond naming, although clearly distinct 
 species from the above. They are:— 
 
 (a.) A small species of nine or ten broad, but not high, simple, carinate whorls 
 —no evidence of the aperture or ornament. It resembles JL carinata in 
 appearance, but possesses at least nine whorls in a length of nine- 
 sixteenths of an inch, whereas in the former there are four in thirteen- 
 sixteenths. 
 
 (6.) A second species of the same general character, but with four or five 
 whorls in the same space—viz., nine-sixteenths of an inch. 
 
 (c.) Astill larger species, two and two and a-half inches in length, with a well- 
 marked band, situated immediately above the suture on all the whorls, but 
 the last one is not preserved, all crossed by oblique striz. 
 
 Family—BELLEROPHONTID. 
 
 Genus—BELLEROPHON, De Montfort, 1808. 
 (Conch. Systématique, i., p. 51.) 
 
 BELLEROPHON STANVELLENSIS, sp. nov., Pl. 15, figs. 11-18. 
 
 Sp. Char. Shell broad-oval, thick, higher than wide, whorls broad and some- 
 what depressed, back generally rounded, and but little excavated on each side of the 
 keel; flanks very obtusely rounded, or even slightly flattened, but in no case angular, 
 Mouth almost semi-circular and much expanded, inner lip spreading over last whorl as a 
 thick wide callosity, and horizontally to join the margins of the outer lip as a lateral 
 
 * See note, p. 199. 
 
290 
 
 expansion. Umbilicus open and deep, visible in a side view, but quite hidden from the 
 front by the alate expansions of the inner lip. Keel narrow and sharp, and but little 
 elevated. On the surface, strie pass directly across the back from the keel to the 
 peripheries above the umbilicus, but do not appear to cross the keel. 
 
 Obs. I, at first, took this to be one or other of the Salt Range (India) species, 
 such as B. Blanfordi, B. affinis, or B. Jonesianus. From the first two, our species 
 differs in the shape of the whorls, from the third by being less globose, and from all 
 three in the nature of the surface ornament, and the exposure of the umbilicus. It 
 appears to belong to the group of Bellerophon hiulcus, Sby., to which it is probably 
 most nearly iia but the mouth is more depressed and lunate, and the callosity deeper 
 and more pronounced. It is the largest Bellerophon I have yet seen from Australian 
 rocks, and is a peculiar form in so far that it unites the characters of more than one 
 group. 
 
 Loc. and Horizon. Stony Creek, Stanwell, near Rockhampton (Zhe late 
 James Smith)—Gympie Beds ; Banana Creek, near Banana, Dawson River (H. Mackay ; 
 Colln. De Vis)—Middle or Marine Series, Bowen River Coal Field. 
 
 Genus—BUCANTA, Hall, 1847. 
 (Pal. New York, 1., p. 32.) 
 
 Bucanta textiits, De Koninck, Pl. 41, fig. 8. 
 
 Bellerophon decussatus, De Koninck (non Fleming), Descrip. Anim. Foss. Terr. Carb. Belgique, 1843, t. 29, 
 f, 2a-d (exel. f. 8a and b). 
 Bucania textilis, De Koninck, Ann, Mus. R. Hist. Nat. Belgique,* 1883, viii., p. 150, t. 41, f. 22-25. 
 
 Obs. There is a very close resemblance between the shell originally called 
 Bellerophon decussatus by De Koninck—but which is not the species of that name of 
 Fleming—and the subject of our figure (Pl. 41, fig. 8). It has been subsequently 
 named Bucania textilis, and is a globular, high shell, with a deep umbilicus. The 
 aperture is large and rather trumpet-shaped, with a thin expanded callosity and a rather 
 shallow sinus. The band is large, projects but little, and is covered with small scales, 
 The entire shell is ornamented with spiral ridges well separated from one another, with 
 finer interpolated ribs, and crossed by strie of growth, which give to it a roughly and 
 irregularly decussated appearance. 
 
 In the Australian shell the umbilicus seems to be rather larger than in the 
 European. 
 
 Loc. and Horizon. Rockhampton District + (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 Genus —PORCELLIA, Leveillé, 1835. 
 (Mém. Soc. Géol. France, ii., p. 39.) 
 
 Porcetria PEaRst, sp. nov., Pl. 15, figs. 7 and 8. 
 
 Sp. Char. Shell small, of five or six whorls; section apparently quadrangular, 
 back slightly convex or almost flat; sides of each whorl bearing prominent, elongated, 
 obtuse’ tubercles, which gradually, and on the body-whorl insensibly, diffuse themselves 
 on to the sides and back. Surface of the whole shell ornamented with spiral and trans- 
 verse raised striw, giving rise to a fine regular reticulation, the points of intersection 
 becoming minutely nodular. 
 
 
 
 * Faune du Calcaire Carbonifére de la Belgique, Pt. 4. 
 + See note, p. 199, 
 
 
 
 
 
 —— 
 
291 
 
 Obs. Although this species has only been met with in fragments, its characters 
 are seen to be at once clear and distinct, the large elongated tubercles and fine 
 reticular ornament rendering it a conspicuous fossil. The tubercles are transversely 
 elongated, and gradually rise from the sides and back of the shell. 
 
 Porcellia Pearsi agrees with P. puzio, Leveillé,* and P. armata, De Verneuil,t 
 in the form and position of the tubercles, and with the former in the reticulation of 
 the surface, but it differs from this particular species in the back of the body-whorl 
 being flat, or practically so. From P. armata the present species may be distinguished 
 by the nature of the ornamenting striw, and the number of tubercles to the whorl. 
 The nearest aliy of P. Pearsi appears to be P. Hdouardi, D’Orb.,t from the Middle 
 Devonian of the Hifel, both as to general form and surface ornament, but here again 
 the back is highly convex and the decussating striz much stronger, whilst the tubercles 
 are less marked and do not project to the extent they do in P. Pearsi. 
 
 Loc. and Horizon. Corner Creek, Great Star River (P. W. Pears)—Star 
 Beds ; Rockhampton District (C. W. De Vis; Colln. De Vis)—Gympie Beds; Banana 
 Creek, near Banana, Dawson River (H. Mackay ; Colln. De Vis)—-Middle or Marine 
 Series of the Bowen River Coal Field. 
 
 Class—PTEROPODA. 
 Order~—THECOSOMATA. 
 Family—CONULARIIDA.§ 
 
 Genus—CONULARIA, Miller (J. Sowerby), 1820. 
 (Min. Con., iii., p. 107.) 
 
 CoNULARIA TENUISTRIATA, McCoy. 
 
 Conularia tenuistriata, McCoy, Ann, and Mag. Nat. Hist., 1847, xx., p. 307, t. 17, f. 7and . 
 A Fi De Koninck, Foss. Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 310, t. 23, f. 2. 
 
 Obs. A small portion of an individual, exhibiting the number of fine transverse 
 strize mentioned by Prof. McCoy as twenty-seven to twenty-nine in the space of half- 
 an-inch, and the upward curve across the broad face, which carries a mesial line, would 
 appear to indicate this species as a Queensland fossil. 
 
 Loe. and Horizon. Gympie (W. H. Rands)—Gympie Beds. 
 
 Conurartia, sp. ind., Pl. 41, fig 10. 
 
 Obs. Another fragment, one and a-quarter inches long, with portions of thirteen 
 wide and flat ridges, divided by similar interspaces. A mesial line traverses the centre 
 longitudinally, representing one of the angles of the shell. Some of the cross ridges 
 are subalternate, and where they abut against the mesial line are slightly grooved. The 
 interspaces are cross-wrinkled, a similar form of ornament being visible in De Koninck’s 
 figure of Oonularia levigata, Morris,|| but no mention is made of it in the description. 
 This is altogether a remarkable fragment, but is far too large for the above species. 
 
 Loc. and Horizon. Gympie (W. H. Rands)—Gywmpie Beds. 
 
 
 
 
 
 
 
 * Mém. Soc. Géol. France, 1835, ii., p. 39, t. 2, f. 10 and 11. 
 
 + Geol. Russia d’Europe, 1845, ii., p. 346, t. 24, f. 3. 
 
 + Hist. Nat. Cephalopoda Acétab. 2me pte., p. 215, Atlas (Cryptodibranches), t. 7, f. 6 and 7, 
 §S. A. Miller, American Pal. Foss., 1877, p. 141. 
 
 || Foss, Pal. Nouv,-Galles du Sud, 1877, Pt. 3, t, 18, f. 9a, 
 
292 
 Class—CEPHALOPODA. 
 Order—TETRABRANCHIATA. 
 
 Family— NAUTILID. 
 
 Genus—NAUTILUS, Breynius, 1732. 
 (Dissert. Phys. Polythalamiis.) 
 
 Obs. Nautilus, or one of its sections, is represented by a decorticated fragment, 
 too imperfect to figure, of a small shell nearly an inch in diameter. There are eight 
 septa visible, and, for the size of the specimen, a large umbilicus. This is the 
 only indication of this genus I have met with in the Queensland Permo-Carboniferous 
 rocks, with the exception of the following peculiar species. 
 
 Loc. and Horizon. Rockhampton District * (0. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 NavrvILus ? AMMONITIFORMIS, sp. nov., Pl. 39, fig. 9; Pl. 41, fig. 9. 
 
 Sp. Char. Shell planorbiform, apparently much depressed, of many closely coiled, 
 convex, uniform, narrow, tube-like whorls in one plane, and, with the exception of the 
 body-whorl, expanding but very slowly. The latter is much flatter and broader than 
 the others, and has lost the tube-like appearance of the inner and older whorls ; aperture 
 unknown. Surface of ali but the body-whorl with angular, direct, transverse ridges, 
 or cost, separated by interspaces of more than their own width, but on the latter they 
 become flattened, depressed ribs, somewhat sigmoidal, presenting a very different 
 appearance. 
 
 Obs. A very peculiar shell, which from its general appearance would seem to 
 be more nearly allied to the Cephalopoda than the Gasteropoda. Not the least peculiar 
 feature is the remarkable regularity of the coil in one plane, whereby the enlargement 
 of the whorls is hardly perceptible until the body-whorl opens out. There are no septa 
 visible, but, on the other hand, the appearance of this shell is quite different to that of 
 any of the Euomphalide, and the sudden expansion of, and change of ornament on the 
 body chamber, cause me to regard it as a Cephalopod. ‘There are traces of a ventral 
 keel, but no spiral striw. The cost on the older chambers are at right angles to the 
 coil, but the ribs on the last chamber assume an oblique direction. The last whorl, and 
 the inner whorls (PI. 39, fig. 9), are frequently found disconnected, when they might be 
 readily mistaken for two distinct species. 
 
 I have been much perplexed with regard to a genus for this fossil, and it is only 
 placed in Nautilus as a matter of convenience, as it is obvious that no real relation 
 exists between the two. As a matter of fact, in outward appearance, these fossils 
 present an exact resemblance to Lituites, especially that section named by Barrande 
 Ophidioceras.t There is the same coil-like form in one plane, tube-like whorls, and 
 separate transverse coste. But JLituites is a Silurian genus and confined to 
 rocks of that age throughout the world. Otherwise, had intermediate Devonian 
 species existed, I should have been tempted to refer the present species to 
 it. On the other hand, this may be one of those extraordinary survivals of 
 an old genus for which the Australian Paleontological record is becoming noted. 
 
 
 
 * See note, p. 199. 
 + Syst. Sil. Centre Bohéme, 1865, ii., Céph. Le. Ser., Pls, 1 107, t. 45, f. 18, 17, 22, 28, 24, &e 
 
293 
 
 It also resembles some species of Zyochoceras. The older and inner whorls of this 
 shell are very like a Cephalopod called Nomismoceras spiratissimum, Holzapfel,* 
 from the Carboniferous Limestone of Erdbach near Herborn, Germany, but the latter 
 species appears to be smooth, and the whorls do not appear to enlarge and expand in 
 the manner shown. 
 
 Loe. and Horizon. Rockhampton District + (C. W. De Vis and Rev. J. LE. 
 Tenison Woods; Colln. De Vis) —Gympie Beds. 
 
 Family—ORTHOCERATID. 
 
 Genus—ORTHOCERAS, Breynius, 1732. 
 (Dissert. Phys. Polythalamiis, pp. 12 and 23.) 
 
 Obs. The remains of this genus appear to be very uncommon in the Queensland 
 Permo-Carboniferous Series, and when met with exceedingly fragmentary. 
 
 A terminal portion of an Orthoceras (Pl. 15, fig. 1), three inches long and rather 
 crushed, was obtained from the Gympie Beds. Its present diameter is one and 
 a-half inches, with obliquely curved transverse striz, rather than ridges, and resembles 
 in general appearance De Koninck’s figure{ of O. striatum, J. Sby., although 
 the longitudinal striation visible on that fossil is not preserved in the present 
 specimen. 
 
 Fragmentary remains of the genus are met with in the Star River Series; one 
 form, without traces of external ornament, possessed distant septa; another had close, 
 fine, thread-like, waved striz ; whilstin a third the ornament was similar, but less waved, 
 coarser, and separated by interspaces with a breadth equal to rather more than the 
 thickness of the striz. 
 
 The Mount Britton Beds have yielded the only specimen yet seen in the round 
 (Pl. 39, fig. 10), showing portions of five chambers, one and three-quarters of an inch 
 long, and one inch in diameter. The chambers are about a quarter of an inch in depth, 
 with a circular section. The specimen is denuded of the test. _ 
 
 In the Collection made by Mr. De Vis are two other Orthoceratites. One consists 
 of seven narrow chambers in a space of twelve-sixteenths of an inch, to some extent 
 flattened like De Koninck’s figure of his Cameroceras .Phillipsii,§ with a vertical linear 
 depression in the middle line. It is ten-sixteenths of an inch wide. 
 
 The other species is represented by two narrow, small shells, about the dimen- 
 sions of O. Martinianum, De Kon.,|| but very delicately transversely striated. They 
 measure two and two and a-half inches respectively, four-sixteenths wide at the 
 distal end, tapering to a fine point. The septa are about one-sixteenth of an inch 
 apart. 
 
 Loc. and Horizon. Gympie (2. L. Jack)—Gympie Beds ; Corner Creek, Great 
 Star River (R. ZL. Jack)—Star Beds; Richards’ Homestead, three miles south-west 
 of Mount Britton Township (2. LZ. Jack)—Middle or Marine Series of the Bowen 
 River Coal Field; Rockhampton District § (OC. W. De Vis; Collnu. De Vis)—Gympie 
 Beds. 
 
 * Dames and Keyser’s Pa]. Abhandlungen, 1889, i., Heft 1, t. 4, f. 8. 
 + See note, p. 199. 
 
 t Foss. Pal. Nouy.-Galles du Sud, 1877, Pt. 3, p. 341, t. 24, f. 2. 
 
 § Ibid., p. 344, t. 24, f. 1. 
 
 || Ibid., p. 348, t. 24, f. 3. 
 
 4 See note, p. 199. 
 
294 
 
 Genus—-GYROCERAS (Von Meyer), De Koninck, 1844. 
 (Descrip. Anim. Foss. Terr. Carb. Belgique, p, 530.) 
 
 GYROCERAS DUBIUS, sp. nov., Pl. 41, fig. 12. 
 
 Sp. Char. Entire shell unknown; terminal portion of bedy-whorl produced 
 and curved rather irregularly; sides convex, but depressed; back or ventral surface 
 concave, bounded by a keel on each side; dorsal surface apparently broad, and not acute, 
 surface bearing sharp, crest-like, obliquely transverse, somewhat semicircular ridges or 
 coste. 
 
 Obs. This interesting fragment would seem to represent a form resembling 
 Gyroceras aigoceras, Miinster,* but with a different curvature, and sharper and more 
 prominent coste. At the same time the very strong likeness it bears to the terminal 
 portion of the shell in Ophidioceras, must not be overlooked. The enlargement at the 
 distal end probably represents the aperture, and in this case the resemblance becomes 
 still more apparent. 
 
 A possible relation with the previous Nautilus ? ammonitiformis, has presented 
 itself for consideration, and would have been entertained had it not been for the great 
 difference between the breadth of the last chamber of the former and that of the present 
 fossil, which renders it almost impossible for the two to be portions of one species. 
 At the same time the irregular curve of G. dubiuvs is unlike the symmetrical outline of 
 G. atgoceras, but only the acquisition of more complete specimens can satisfactorily 
 explain the relation of these obscure and indifferently preserved shells. 
 
 Loc. and Horizon. Rockhampton District + (The late Rev. J. H. Tenison Woods ; 
 Colln. De Vis) —Gympie Beds. 
 
 Family—GONIATITIDA. 
 
 Genus—GONTIATITES, De Haan, 1825. 
 (Mon. Ammonites et Goniatites, p. 39.) 
 
 GONIATITES MICROMPHALUS, Morris. 
 
 Bellerophon micromphalus, Morris, Strzelecki’s Phys. Descrip. N. 8. Wales, &c., 1845, p. 288, t. 18, f. 7. 
 Dana, Geology Wilkes’ U. S. Explor. Exped., p. 708, Atlas, t. 10, f. 6. 
 Goniatites Waeonpiice De Koninck, Foss, Pal. Nouv.-Galles du Sud, 1877, Pt. 3, p. 339, t. 24, f. 5. 
 - 6 Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 304. 
 
 Obs. ‘Two specimens of this species have been collected by my Colleague, both of 
 them casts, without any -trace of shelly matter remaining. The form of the shell and 
 character of the umbilicus in the Bowen River Coal Field specimens correspond quite 
 well with Professor Morris’s description and figures, but the depth of the body-whorl 
 near the mouth is not so great, although the disparity is greater in one of our specimens 
 than in the other. However, this need be dwelt on less, since Prof. Dana has given 
 such a figure ¢ of G. micromphalus, and on examining those in the Strzelecki Collection 
 the same aperture was found to exist in some of the specimens there. 
 
 Loc. and Horizon. Head of Pelican Creek, near Mount Divlin, Bowen River 
 (R. L. Jack)—Maiddle or Marine Series, Bowen River Coal Field. 
 
 * Ann. Mus. R. Hist. Nat. Belgique, 1880, v., t. 32, f. 4 (Faune du Calcaire Carbonifére de la 
 Belgique, Pt. 2.) 
 
 + See note, p 199. 
 
 + Geology Wilkes’ U, 8, Explor, Exped,, Atlas, t. 10, f. 6a 
 
 
 
295 
 
 GonrIATITES, sp. ind., Pl. 15, fig. 5. 
 
 Goniatites, sp. ind., Etheridge fil., Proc. R. Phys. Soc. Edinb., 1880, v., p. 305. 
 
 Obs. A second species is present in the Bowen River Beds, differing from 
 G. micromphalus in having a very much sharper back. It appears to be nearer to 
 G. striatus, Dana,* than to Morris’s species. A sharp-backed Goniatite has also been 
 found at Gympie. It is much sharper and narrower than G. micromphalus, and is 
 interesting from its locality. 
 
 Loc. and Horizon. Rosella Creek, two miles above Havilah Paddock (R&. L. 
 Jack). This is an important fossil, as it is another of those occurring in a marine 
 band in the Upper or Fresh Water Series. Gympie (R. L. Jack). 
 
 GONIATITES PLANORBIFORMIS, sp. nov., Pl. 41, fig. 9. 
 
 Sp. Char. Whorls numerous, at least six, increasing in size very slowly and in 
 one plane, coil-like or planorbiform, very slightly convex; no umbilicus visible; test not 
 preserved, but surface plain in casts; lobes and saddles nearly equal, but the latter 
 rather the more pointed ; two chambers occupy about the space of seven millimetres. 
 
 Obs. The preservation of this shell only in the form of casts renders it very 
 difficult to assign it reliable characters, but the chief and striking point is its very 
 compactly coiled and planorbiform aspect. The largest specimen observed measures 
 one and a-half inches in diameter, the whorls increasing in size very slowly. 
 
 The septa are very rarely seen, the specimens having very much more the 
 appearance of a tightly and flatly coiled Euomphaloid shell than a Goniatite. The 
 species is of the type of, and nearly allied to, Goniatites clymenieformis, De Koninck,t but 
 the body-whorl of the latter is much broader than in ours. A somewhat similar shell 
 is Huomphalus sancti-sabe, Roemer,t from the Carboniferous of Texas, which may as 
 well be a Goniatite as a Euomphalus, for all the evidence there is to the contrary. 
 
 The sutural convolutions do not well correspond with any of the recognised 
 groups of Goniatites, but they approach nearest to those of the subdivision Carbonarii in 
 Beyrich’s classification. Neither have I been able to locate this species in either of 
 the sections proposed by the Brothers Sandberger on similar anatomical structure. 
 
 Loe. and Horizon. Lake’s Creek, near Rockhampton (The late James Smith) ; 
 Rockhampton District § (The late Rev. J. E. Tenison Woods ; Colln. De Vis)—Gympie 
 Beds. 
 
 GontTATITES, sp. ind., Pl. 15, figs. 14 and 15. 
 [Compare G. striatus, J. Sby., Min. Con., 1814, i., p. 115, t. 58, f. 1.] 
 
 Obs. A moderately large Goniatite, in a bad state of preservation, but much 
 larger and stouter than G. micromphalus, was obtained by the late Mr. James Smith. It 
 is viewed partly in the round, partly in section, from the manner in which the stone has 
 been fractured. It clearly belongs to the group of the above species, the externa] 
 ornament, so far as preserved, corresponding with that of the type of G. striatus in 
 the Sowerby Collection.|| I think it is even possible to recognize, in places, the minutely 
 delicate cross-bars between the regular spiral raised lines of the surface. The course 
 of the septa is identical with that of Sowerby’s species, and strong varices of growth 
 are also here and there visible across the back of the specimen. The septa apparently 
 have four folds, sharp and angular. The umbilicus is small and regular as in the type 
 and all the volutions hidden. 
 
 * Loc. cit., f. ba and 6. 
 + Faune Calc. Carb. Belgique, Pt. 2, 1880, t. 49, f. 12. 
 t Kreidebildung von Texas, 1852, t. 11, f. 5a and 5, 
 
 § See note, p. 199. 
 || Natural History Museum, London, 
 
296 
 
 Mr. W. H. Rands has found a second specimen, convex and round, and generally 
 like the above. It has a small umbilicus, but the other characters are obscure. 
 
 Loe. and Horizon. Training Wall Quarries, Rockhampton (The late James 
 Smith); Hawkins’ Gully, Kariboe Creek, Kroombit Diggings, Port Curtis (W. 4H. 
 
 Rands)—Gympie Beds. 
 
 Sub-Kingdom—VERTEBRATA. 
 Class—PIScES. 
 
 Order—CHONDROPTERYGII. 
 Family—COCHLIODONTID &. 
 
 Genus—DELTODUS, L. Agassiz, 1859, M.S. 
 (Enniskillen Collection. )* 
 
 DELTODUS ? AUSTRALIS, sp. nov., Pl, 89, fig. 11. 
 
 Sp. Char. Oblong-triangular, insensibly flattening towards the broader or 
 anterior end. The outer side is thickened, and obtusely rounded, the outer or base thinner 
 and sharper. Anterior margin gently rounded, the posterior end gradually acumin- 
 ating, and more or less obtusely so. The surface gradually decreases towards the basal 
 and anterior margins, and is traversed almost medianly by a rather curved, wide, deep 
 sulcus, narrower at the basal than the outer end, and followed in the direction of the 
 anterior end, by two other parallel and indistinct depressions. Structure open and 
 porous. Section semi-circular, abruptly so on the outer side. 
 
 Obs. With the exception of the Zomodus convexus, Ag., figured by Prof. De 
 Koninck, from the Permo-Carboniferous of New South Wales, this is the only Cochlio- 
 dont known to me from this portion of the Australian Paleozoic rocks. JI do not feel 
 at all certain that the reference to Deltodus is a correct one, but in the unsatisfactory 
 state of our antipodean scientific libraries, I am unable to make a more exact determina- 
 tion. If a species of this genus, it approaches D. aliformis, McCoy, but is much more 
 regular in outline, and lacks the contracted posterior end of that species. 
 
 Loc. and Horizon. Rockhampton District | (C. W. De Vis; Colln. De Vis)— 
 Gympie Beds. 
 
 Order—GANOIDEI. 
 Family—PALZONISCIDA. 
 
 Remains of a Paleoniscid fish have been presented to the Mining and Geological 
 Museum, Sydney, by Mr. C. T. Musson, F.L.S. “from a ridge half a mile from and 
 to the north of the Bogantungan Railway Station,” Drummond Range (= Star Beds).f 
 From the same locality the late Mr. James Smith made a large collection of fish- 
 remains, which I have not yet had an opportunity of examining. 
 
 Mr. Rands has also recently discovered the remains of a fish in the Star Beds 
 near Lornesleigh Station.§ It certainly belongs to this family, and, so far as the want 
 of the head will permit an opinion to be formed, it appertains to the genus Palgoniscus. 
 
 * Fide Morris and Roberts, Quart. Journ. Geol. Soc., 1862, xviii., p. 100; defined, Newberry and 
 Worthen, Illinois Geol. Report, 1866, ii., p. 95; A. Smith Woodward, Cat. Foss. Fishes Brit. Mus., 1889 
 Pt. 1, p. 195. 
 
 + See note, p. 199. 
 t Etheridge, junr., Records Geol. Survey N.S. Wales, 1890, Vol. ii., Pt. 2, p. 71. 
 
 § Report on the Cape River Gold Field. Brisbane: by Authority : 1891. 
 
297 
 
 INSERT: SEDIS. 
 TRACKS AND MARKINGS. 
 
 Arentcoritss, Salter,* Pl. 8, figs. 2 and 3. 
 
 Obs. The late Mr. James Smith found in the Stanwell Building-stone, a 
 number of vertical tubes, with trumpet-mouth-shaped openings, the resemblance of 
 which to Salter’s Arenicolites he called attention to on the labels of his specimens. 
 
 The tubes are vertical, straight, and at right angles to the bedding of the 
 ferruginous sandstone in which they occur, sometimes single, at other times in pairs. 
 When double they are parallel to one another, one end of each tube expanding into a 
 trumpet-mouth-shaped aperture. The walls, internally appear to have been concentri- 
 cally ridged, when the sediment with which they have been filled is removed. The 
 latter is of a finer consistency than the surrounding matrix, and of a different shade of 
 colour. 
 
 The tubes of the Stanwell Building-stone are much larger than those of the 
 English Cambrian rocks, described by Salter, but they more closely resemble, both in 
 size and appearance, others from the Durness Limestone,+ figured by the same Author. 
 
 The nature of these burrows is extremely doubtful, but I do not believe in the 
 theory which ascribes them to the action of worms. That they are the burrows of some 
 animal is unquestionable, but an explanation should be looked for amongst the 
 Mollusca rather than the Annelida. Very similar burrows are produced, for instance, 
 by the Razor-fish (Solen). They do not partake of the nature of those elongated 
 tubes for which Prof. James Hall suggested the name of Scolithus. 
 
 Loc. and Horizon. Stanwell Building-stone, near Rockhampton (The late 
 James Smith)—Gympie Beds. 
 
 BuRROWS. P 
 Pl. 8, fig. 4; Pl. 39, fig. 1; Pl. 44, figs. 15-18. 
 
 Obs. I am indebted to Mr. C. W. de Vis, of the Queensland Museum, for the 
 peculiar bodies about to be described. They occur in a shale which has undergone 
 much alteration, and become exceedingly hard, brittle, and cherty, and they further 
 present a different appearance as they are seen in this matrix, or its weathered and 
 semi-decomposed equivalent. I have not been able to absolutely detect the bedding in 
 this rock, but appearances point to these markings being parallel to it, or, perhaps, 
 cutting it at an obliqueangle. In the decomposed material they present the appearance 
 of straight or slightly-curved tubes, which dilate somewhat at their distal ends, or 
 enlargements may take place during the course of the burrow. These passages are 
 filled with a material resembling the surrounding matrix in colour and consistence, but 
 broken up into segments, or divided into a series of infundibuliform divisions after the 
 manner of the chambers of a multilocular shell. -In this condition these curious 
 remains appear under two aspects—First, as infilled tubes preserved in the round, 
 each segment fitting into its neighbour, and weathering out separately one from the 
 other: Secondly, when the surface of the matrix has been removed by weathering, 
 the outline of the tube is destroyed, but the segments are left in relief as a number of 
 disjointed and apparently moniliform bodies, and in this condition resembling many 
 tracks, which have from time to time been erroneously referred to worms and other 
 improbable organisms. 
 
 * Quart, Journ. Geol. Soc., 1859, xili., p, 204. 
 + Loe. ctt., 1859, xv., t. 18, f. 29 and 30, 
 
298 
 
 On the weathered surfaces of the hardened and undecomposed shale, the remains 
 of these burrows present a most peculiar appearance, all traces of the tube having 
 disappeared, whilst the infilling portions, often, in this case, of a different colour to the 
 surrounding matrix, are left as a series of more or less disjointed, infundibuliform stains. 
 This is the longitudinal aspect, but when seen in section the circular outline is quite 
 apparent, and as both longitudinal and transverse sections are visible on the same 
 specimen no doubt can be entertained of their connection with one another. In our 
 present limited knowledge of the nature of the numerous tracks and markings found on 
 the surfaces of the older rocks, it is difficult to offer a reliable explanation of these bodies. 
 It has been customary to make the Annelida a kind of refuge for the destitute in such 
 cases, but the writings of the late Prof. Ferdinand von Roemer, Mr. Nathorst, and others 
 have probably given the death-blow to this loose method of generalisation. A general 
 epitome of the subject will be found in an article by Prof. H. A. Nicholson and the 
 Writer,* but no better explanation of how a large number of these tracks are formed has 
 been offered than the lucid and exhaustive description by the late Albany Handcock of 
 vermiform markings in the Carboniferous Limestone of the North of England.+ This 
 eminent Naturalist has suggested the analogy of his vermiform markings to the burrows 
 of certain Amphipod Crustaceans, named Avréyeria arenaria, Bate, and Suleator 
 arenarius, made in shore-sand under his own eyes. Speaking of certain of the fossil- 
 tracks, be says :—‘‘ Full-sized specimens are half an inch wide, and are composed of a 
 series of nodules, which give them an articulated appearance. The nodules, which vary 
 a little in size, are usually about half an inch long, and are not very symmetrically or 
 regularly formed. Consequently the surface has generally an imperfect or worn 
 character. The extremities are not often seen; they are abruptly and irregularly 
 rounded.” 
 
 These remarks were supplemented by the following :—‘ The specimens 
 are characterised, as we have seen, by a remarkable nodulous or articulated Spyeetiiw 
 which has been supposed to indicate the presence of rings of some Annelide ; and, indeed, 
 were it not for the light derived from the Crustacean tracks on our shores, it would not 
 be easy to conjecture a more plausible explanation. We have seen, however, that a 
 variety of the track of Kréyeria arenaria has the ridge of sand thrown up, broken into 
 nodules, giving to it a beaded character. This, on a small scale, has a considerable 
 resemblance to these nodular forms. But a much nearer approximation is found with 
 nodulous tracks of Suleatorarenarius. . . . . . Itmay therefore be assumed that 
 the animal which made these nodulous tracks, like our small Crustacean, pushed along in its 
 path, step by step, resting awhile after each advance, but that, instead of moving in each 
 horizontal plane, it alternately rose and sunk a little ; consequently, a series of nodules 
 was produced, and the track acquired its peculiar articulated appearance. This explana- 
 tion is strengthened not a little when we look at the side view of the cast of this track. 
 The nodules are then distinctly observed to be imbricated, and to pass, very much 
 inclined, right through the substance from top to bottom.” 
 
 Without implying that the Rockhampton markings are produced by Amphipods, 
 these quotations are simply given to show that it is not necessary to call in the aid of 
 the Annelida for their explanation. The only Crustaceans known to occur in these beds 
 are Trilobites, but the tracks are not such as have been hitherto ascribed to these 
 animals. Other organisms are capable of causing such raised tracks, as evinced by 
 
 * Mon. Sil. Foss. Girvan in Ayrshire, 1880, Pt. 3, p. 304. 
 
 + ** Remarks on certain Vermiform Fossils found in the Mountain Limestone Districts of the North 
 of England.” Ann. and Mag, Nat. Hist., 1858, ii., p. 443; Trans, Tyneside Nat. Field Club, 1858, iv., Pt. i, 
 yen Abie. 
 
 
 
299 
 
 the trail of the common British Purpura, figured by Professor H. A. Nicholson and the 
 Writer.* It is therefore clear that, between the Crustacea and Mollusca, there is a 
 wide field for speculation as to the origin of these peculiar burrows. 
 
 In their disjointed nature, they bear considerable resemblance to the so-called 
 Carboniferous worm-track, elevated into a genus by the late Mr. G. Tate, of Alnwick, 
 under the name of Eione.t When seen in a weathered disjointed state (PI. 8, fig. 2) 
 there is a very marked similarity to his Hione moniliformis.t 
 
 In the memoir quoted above, Mr. Handcock speculated as to his tracks or 
 burrows being made by Trilobites, and appeared to favour such an explanation. Those 
 under description, however, would not be large enough to accommodate the Phillipsia 
 and Griffithides, hitherto found in the Permo-Carboniferous rocks of Queensland. 
 
 -Finally, it may be pointed out that these burrows appear almost identical 
 with the so-called worm-tracks from the black slates of the Happy Valley, north of 
 Nelson, New Zealand, and figured in the account of the “ Novara’’ Expedition.§ 
 
 Loc. and Horizon. Athelstane Range, near Rockhampton (The late James Smith); 
 
 Rockhampton District || (C. W. De Vis; Colln. De Vis)—Gympie Beds. 
 
 *Mon. Sil. Foss. Girvan in Ayrshire, 1880, Pt. 2, p. 317, f. 11. 
 
 +The Geology of Beadnell, in the County of Northumberland, with a description of some Annelids of 
 the Carboniferous Formation, Geologist, 1859, ii., p. 59. 
 
 + Loe. cit., p. 62, t. 2, f. 6. 
 
 § Reise Oester. Fregatte ‘‘ Novara,” 1857-59, Geol. Theil., Bd. i., 2 Abth., 1865, . 7, f. 5. 
 
 || See note, p. 199. 
 
CHAPTER XXIII. 
 
 THE TRIAS-JURA SYSTEM. 
 LOWER (BURRUM) FORMATION. 
 
 On a higher horizon than the Permo-Carboniferous System and on a lower than 
 the Ipswich Formation, the great series of coal-bearing rocks known as the Burrum 
 Coal Field is met with. This Coal Field extends along the eastern coast line, from Point 
 Cartwright on the south at least to Littabella Creek on the north, and stretches inland 
 for an average distance of twenty-five miles. Its area may be roughly estimated at 
 three thousand square wiles. 
 
 Divided from the main area of the Burrum Coal Field by a mass of granite, a 
 small area supposed to belong to the same period is met with at the south end of Rodd 
 Bay. 
 
 Still another area, believed to be of the same age, occurs in the Valley of the 
 Styx, at the southern end of Broad Sound. 
 
 The Burrum Formation has been traced southward to near Point Cartwright, 
 where it is no great distance from the northern end of the Ipswich Coal Field. The 
 two coalfields are separated by a protrusion of slaty rocks, which may be supposed to 
 belong to the Gympie Formation. It is to be regretted that the relation of the two 
 fields cannot be seen at this point. All that can be stated is that they apparently are 
 characterised by a distinct fauna and flora. 
 
 The Burrum Coal Field is characterised by a very meagre flora and a fauna 
 represented only by one species of Corbicula and one of Rocellaria. The latter are 
 both new species. Of the flora four species occur also in the Ipswich Formation, while 
 six other species are confined (so far as our Collections show) to the Burrum F[or- 
 mation. 
 
 Mr. Gregory referred to the finding of Glossopteris above the Upper or Beau- 
 fort Seam of Coal. Mr. Rands observed in his Report of 1886 that he had failed to find 
 Glossopteris. In his Annual Report for 1886, however, he stated, ‘‘I have found several 
 specimens of Glossopteris Browniana amongst stone from the Briton Shaft.” My 
 Colleague, however, is not satisfied that Glossopteris really occurs in these beds. Such 
 
 of Mr. Gregory’s and Mr. Rands’ specimens as have come under his notice he regards 
 
 as Teeniopterid plants. 
 
 The whole country covered by this formation is low and flat, and is characterised 
 by a poor soil and stunted vegetation. The latter circumstance is, however, due to a thin 
 covering of a more recent formation which overlies it unconformably. 
 
 Distinct from the thin covering and certainly older, is the group of fossiliferous 
 sandstones known as the Maryborough Beds, which are placed on the same horizon as 
 the Desert Sandstone (which sec). The relation of the Maryborough Beds to the 
 Burrum Beds, although obscure, is believed to be that the former rest unconformably 
 on the latter, and that a fault (which, however, is not seen) must account for the fact 
 that the lowest of the Maryborough Beds, after dipping, do not rise on the other side. 
 Their apparent conformability to the Burrum Beds must be deceptive, as even if the 
 latter were equivalent to the uppermost members of the Ipswich Formation, the whole 
 of the Rolling Downs Period is unrepresented. Mr. Rands sends me (in a letter dated 
 16th September, 1889) the Section reproduced in Plate 46, fig. 3, explanatory of this 
 relation. 
 
 
 
301 
 
 The Burrum Beds themselves lie unconformably on the Gympie Beds (Permo- 
 Carboniferous), as is shown by the Section, Pl. 50, fig. 2, taken from a Report by Mr. 
 Rands,* who remarks :— 
 
 “The actual junction of the Gympie Beds with the [Burrum] Coal Measures is 
 concealed by sandy country. At the southern boundary of the Coal Measures the 
 relation of these beds to one another is better seen on the Maryborough and Gympie 
 Railway, about two miles south of the Curra Station. There is a hard porphyritic rock 
 containing crystals of felspar, hornblende, and miea, in the cutting fifty-one miles from 
 Maryborough. Laminated sandstones and shales belonging to the Burrum Beds occur 
 in a cutting fifty and a-half miles from Maryborough. They dip N.W. at 6°, and 
 overlie the porphyry, which here is more of the character of a white felsite. In the 
 cutting at fifty-one and a-half miles from Maryborough, white felsite occurs again, 
 while, ten chains further south, the upper shales of the Gympie Series come in, dipping 
 E. 40° N. at 45°. A small ‘sheet’ of felsite is seen in these shales, about two 
 chains further south, and a larger sheet of it about one and a-half miles south of that 
 again. The Gympie shales do not appear to have been baked or altered by this rock, 
 and I am of opinion that the felsite is interbedded with the shales. But supposing the 
 felsite to be intrusive in the shales, it was intruded before the Burrum Beds were 
 deposited, otherwise we should find it intruding these beds also, which is not the case. 
 In either case, therefore, the unconformability of the Burrum and Gympie Beds is 
 manifest.” ; 
 
 Within certain limits, therefore, the age of the Burrum Beds is fixed by 
 stratigraphical evidence. They are newer than the Permo-Carboniferous, and older 
 than the Upper Cretaceous. 
 
 On the western edge of the field the strata, which in the type district are 
 unaltered, and but little disturbed, become inclined at high angles, and altered into 
 micaceous slates, which are veined with quartz, and finally rest upon granites. 
 
 Prior to the date (1886) of my “ Handbook of Queensland Geology,” the chief 
 sources of information regarding the Burrum Coal Field were Mr. A. C. Gregory’s 
 two Reports,t and passages in the Rev. J. E. Tenison Woods’ “Coal Resources of 
 Queensland.”+ Since that date, Mr. Rands has furnished two Reports,§ dealing with 
 the stratigraphical geology of the series in detail. The description which follows is 
 mainly compiled from these writings, with such additions as I have been able to make 
 from a limited personal knowledge of the district. 
 
 In the immediate neighbourhood of the town of Howard, which is the centre of 
 mining operations, the strata dip with great regularity to the north-east, at an average 
 angle of about 12°, and do not appear to be disturbed by faults of any magnitude. 
 From his surveys, Mr. Rands has compiled the following section :— 
 
 
 
 IG Bins 
 
 Brown and grey sandstone ... aks oe te a’ “Gi we 740) 0 
 Shales with beds of sandstone a ze is ae ae a OGel0) 
 Coal ee =e ee Se ne eae a T 
 
 Bripce SEAM Shale ... ee 3h ne are Ag oe L, 
 Copal ae “5 Pek: ov oe see eee One 
 
 Carried forward se Bae ane a Af soe, LENS oe 
 
 * Report on Tiaro District : The Coal Measures, &c. Brisbane: by Authority : 1890. 
 
 + On the Geology of part of the Districts of Wide Bay and Burnett. Brisbane: by Authority: 1875. 
 And Report on the Burrum Coal Field. Brisbane: by Authority: 1870. 
 
 + Brisbane: The Government Printer, 1883. 
 
 § Report on the Burrum Coal Field. Brisbane: by Authority ; 1886. And Report on Tiaro District : 
 The Coal Measures, &c. Brisbane: by Authority: 1890. 
 

 
 Ft. in. 
 
 Brought forward +e ae ae ze fn eel oys 
 
 Shales with thin Coal-seams pe a ann ae = LUO 
 Coal, LapHam or ToRBANELEA SEAM se Nie 56 4ft. llin. to 2 0 
 Shales .. is ie ie. he “e oe ws Ae on cy 0) 
 Coal, Be RRUM Gaile nee Re A totus 
 Shales with thin beds of candatons and a thin seam of Gate pelo OREO 
 Coal, Watson’s SEAM oe a. oe Mee ee Hier ee 
 Shales... a es att vai ae BEE Ar ue ane. YON 16, 
 Sandstone... Ae Pee: ad = oie “at ean ». 150 O 
 Coalmaer. ace ae Bee aa Kee a oe Lon 
 Sandstone ae Bhalot, ee a Soke ar ee aso EO) 
 Coal, said to be es are Ric = os nae i sae oe Xe 
 Sandstone... ies nee a: nity mii ae LAO 
 Coal, Nort Fipwny Smit ne on + an a ae eee, 
 Sandstone... a we sar ne 88820 
 Ooal, three thin ESTES 2 * 4 cnehee hie ee "Be tn pee Oe 
 Sandstone... ie ae - Kee ne ee sey te) 
 Coal, GLENESK Soret) mf - = ae ae aes epee 2h) i.) 
 Total ae ae 1,015 O 
 
 That the above form only a small merron af Me ota nes of the Coal Measures 
 is evident from the map attached to Mr. Rands’ Report. A copy of the map on a 
 reduced seale is given in Pl. 47. The strata continue to rise in the same direction and 
 at the same angle for at least two and a quarter miles up the streams which make 
 sections to the south-west, before any inversions of dip or want of evidence would lead 
 us to doubt that we are crossing the successive outcrops of similar strata. Probably the 
 total thickness of strata beneath the Glenesk Seam is not less than three thousand feet, 
 or, say, four thousand feet of strata below the horizon of the Bridge Seam. 
 
 It may be mentioned that there are some discrepancies between Mr. Gregory’s 
 and Mr. Rands’ readings of the section ; thus Mr. Gregory gives the distance between the 
 Lapham and Burrum Seams as fifty five and Mr. Rands as thirty five feet. Between 
 the Burrum and Watson’s Seams, Mr. Gregory gives one hundred and Mr. Rands one 
 hundred and fifty feet; and between Watson’s and the North Hartley Mr. Gregory gives 
 five hundred and Mr. Rands two hundred and sixty eight feet. I presume that Mr. 
 Rands, being in possession of later information, is more correct in these details. A 
 bore at Torbanelea, quoted in Mr. Rands’ Annual Report for 1886, gives the position of 
 the Watson Seam as one hundred and fifty feet above the Burrum. 
 
 Mr. Rands gives the following particulars regarding the Torbanelea Mine :— 
 
 “ The pit is sunk through the Lapham or Torbanelea Mine down to the Burrum 
 Seam, cutting the former at eighty five feet and the latter at one hundred and ten feet. 
 Work was at first started at the Lower or Burrum Seam, but it has been abandoned 
 for the time being to work the Lapham Seam, which is reached by a crosscut put in 
 from the former. The Lapham is a harder and better coal, especially for gas-making 
 purposes. The Burrum Seam is here three feet eleven inches thick, with a band of 
 shale seven inches thick. The roofisa grey shale and is fairly good. ‘The coal is 
 friable. 
 
 “The Lapham Seam is thicker, and is a more solid and brighter coal. It is six 
 feet two inches in thickness, including a band of black carbonaceous shale one foot 
 three inches thick in the middle. The roof is of black shale. Experiments conducted at 
 Melbourne prove this to be a good steam coal. Two tons of coal evaporated 3,900 
 gallons of water, whereas two tons of the best Newcastle (N.S.W.) coal evaporated 
 
303 
 
 only 3,200 gallons, or in a ratio of 82 to 74. The manager of the Maryborough gas- 
 works gave me the following returns from twenty months’ actual work with the coal 
 from this seam :— 
 
 Gas... en a 10,200 cub. ft. per ton of Coal. Candle power, 14°73. 
 Coke ... aes BC 1,460 lb. on * (65 per cent.) 
 
 Pare oe, é sek 10°65 gallons _,, 3 
 
 Ammoniacal Recor ae 16°0 *. ” » 
 
 “The Queensland Coal Company’s shaft gave the following sections :— 
 
 oa 
 i=) 
 
 Coal ... 
 
 Black shale 
 
 Coal 
 
 Fireclay ‘ , 
 Sandstone with ronsione bane <a 
 Light clay 
 
 Coal ... 
 
 Black shale .., 
 
 Hand band of Sveclay 
 
 Shale and ironstone., 
 
 Shale with ferns 
 
 Sandy clay 
 
 Coal ; 
 
 Fireclay and bands of pousione 
 Dark coaly shale and ironstone ... set ht oa ses 
 Black shale ... 
 
 Coal 
 
 Fireclay 
 
 Striped sandstone a ironstone 
 Striped sandy shale and ironstone 
 Shale .., 
 
 Coal ... 
 
 Shale . 
 
 Coaiey,.; 
 
 Shale ., .y oy oy exe 
 Coal an. aes Eh le ger nee 
 Fireclay c 
 Coaly shale Ss 
 
 Shales,., nf oes 
 
 Coal ... 
 
 Fireclay F 
 
 Fireclay with nodules 
 
 = il 
 SCWOMANNDOKRPWADWHE 
 
 = 
 
 — 
 AWwONTNDROKARFKRPOBRNWAHP WOOP 
 
 _ 
 WRORP RF WOPKFRrFOWNERONADROWHEAROOHNWOOOR 
 
 
 
 Total ae Lae an He ey oe Aa Peecode 8 
 
 ‘* The seam being worked varies very much in thickness. In the north-westerly 
 level, at four hundred and thirty feet from the pit bottom, it measures— 
 
 ~ 
 
 ONNOBLROB 
 
 Shale... 
 
 Coat... 
 
 Shale ... ae 
 
 Coalaure me hes As ok we 
 
 Shale ... Ss ce wt i. ae 
 
 Coal ve ee 
 
 Fireclay ea eae as aa — - asa 
 
 SOrorcoo? 
 
304 
 
 ‘Tn the same level, seven hundred and fifty feet from the pit bottom, the coal 
 measures three feet six inches, without any intervening shale. The same seam was 
 worked in Whitley’s shaft.” 
 
 Mr. Rands conjectures that the seam worked in the Company’s mine may be the 
 Lapham Seam. 
 
 The Howard, or Beaufort and Howard Seam, “ four feet five inches thick, with only 
 a thin band of shale,” was worked from shafts fifty feet in depth. The seam “lies 
 probably above the seam worked by the Company’’ [Rands]. Mr. Gregory places the 
 Beaufort Seam thirty feet above the Lapham. 
 
 The Glenesk Seam has been worked from a shaft one hundred feet in depth. It is 
 from eighteen inches to two feet in thickness. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 ANALYSES. 
 Volatile : i 
 Ane olatile | Fixed Specifi 
 -—— Water. eee oD Ohrbon. Ash. Sulphur. Gravity. Coke. 
 1, Whitley’s Shaft (Q.C. Co’s Seam) ee 26°6 68°4 50 
 2. Beautort Seam (Beaufort Shaft)... Be 315 64°0 4:5 
 3. Burrum Seam (outcrop) ste ey 29'8 62:2 8:0 
 4. Q. C. Co’s. Seam ... fee sie 2°50 30°35 64°30 2°50 0°35 1°24 66'80 
 (grey) 
 5. Lapham or Torbanelea Seam] 2°00 28°00 61°60 8 00 0:40 131 69°60 
 (Torbanelea Colliery, bottom (grey) 
 coal) 
 6. Ditto (top coal) .. .. «| 225 | 2915] 6650] 210 |... 1:26 | 68°60 
 (grey) 
 7. Burrum Seam (Torbanelea Col-| 2°75 28:00 | 66°55 3°25 0°45 1:27 68°60 
 liery) (reddish) 
 8. Torbanelea Seam ... Ate ae 0:10 27:00 69°96 2 04 090 
 
 
 
 
 
 
 
 
 
 
 
 Analyses Nos. 1, 2, and 3 are by Mr. Gregory ; Nos. 4, 5, 6, and 7, by Mr. Rands; and No. 8 by 
 Dr. D. Marsh, quoted by Dr. J. R. M. Robertson in a Report on the Torbanelea Mine. 
 
 On the coal-seams of the Burrum field generally, Mr. Rands remarks :— 
 
 “The analyses of the coals from the Burrum would show that, with reference to 
 the volatile hydrocarbons, of which, of course, a high percentage is necessary for gas- 
 making purposes, they are not quite as good as the Newcastle coals (New South Wales). 
 Fourteen samples of the latter averaged 37°55 per cent. of volatile hydrocarbons, 
 including water; while the average of seven samples from Burrum is 31°5, that is also 
 taking the hydrocarbons and water together. 
 
 “The ash, which represents so much of worse than useless matter, is by no means 
 high; the highest result being 8 per cent., and lowest 2:1 per cent., the average being 
 4°6 per cent., as against an average of 4°97 per cent. in the Newcastle coal (New South 
 Wales). It should be mentioned that the Burrum samples are from shallow depths, 
 where the ash is generally higher. The ash is of avery light red or grey colour. 
 
 “The sulphur, averaging 0°4 per cent. in the three samples in which I determined 
 it, is very low indeed, and the coal will compare favourably in that respect with coal 
 from any part of the world. Unfortunately, however, in all the analyses of the 
 Burrum coals hitherto made, the sulphur has not been determined. The percentage of 
 this constituent is most important in coals used for gas-making. Freedom from 
 sulphur, too, is a great advantage in many metallurgical processes. 
 
 “The cokes from the Queensland Collieries Company’s seam, the Lapham or 
 Torbanlea seam, and the Burrum seam, are all good, coherent, dense cokes; that from 
 the first-named being the densest. The Burrum coal is not so good a steam coal on 
 account of its tenderness, it being very easily broken up by attrition.” 
 
 
 
305 
 
 Several seams of coal are seen in Cherwell Creek, about four miles to the north- 
 west of Howard, as well as in the Isis and Gregory Rivers. 
 
 South of Maryborough the same formation has been mapped and reported on 
 by Mr. Rands. It is separated from the Permo-Carboniferous rocks by a line running 
 south-east from the heads of Ooramera Creek to the Mary River, south of the mouth 
 of Hookey Creek, and thence eastward to Curra Creek. From Curra Creek the line runs 
 north-eastward till it bends round the spurs of Mt. Goomboorian, on which the Neerdie 
 Antimony Mines are situated. Thence the line runs south-south-east to the coast at 
 Point Cartwright. The strata are disposed in a trough, of which the synelinal 
 axis, roughly speaking, coincides with the line of the Maryborough and Gympie 
 Railway. 
 
 In the Tiaro District, the formation is much more disturbed by faults and 
 intrusive rocks than in the Burrum District. The direction and degree of dip are 
 seldom the same over any large area. In many places dykes and masses of intrusive 
 rocks come up through and disturb the coal strata. The Kannagan Range, near 
 Kilkivan Junction, consists entirely of felsite-porphyry. An intrusive mass of horn- 
 blende and felspar-porphyry occurs near Tiaro. Near Aurora Plantation a large dyke 
 of porphyritic rock forms a bar across the Mary River, and a similar rock occurs in a 
 railway cutting north of Mungar. A volcanic agglomerate is seen on the Railway 
 tweuty three and a half miles from Maryborough. A mass of micaceous granite occurs 
 on the eastern slope of Mt. Bopple. The granitic mass of Teebar abuts to the north 
 against both the Burrum and the Gympie Beds. 
 
 The strata consists of conglomerates, sandstones, shales and clays, with beds of 
 coal, and are, on the whole, very much similar to those of the Burrum District. They 
 are full of plant-remains, which, however, are generally not well preserved. The dip 
 of the strata is generally very high, varying from 25° to 48°. 
 
 In Bull’s Selection (No. 1537), near Gunalda, a seam of bright steel-grey 
 anthracitic coal, eighteen to twenty inches thick, was cut in a shaft at a depth of forty 
 one feet. The coal and other strata dip W. 20° S. at a low angle towards the felsite 
 of the Kannagan Range. The shales have been baked, and the greater part of the hydro- 
 carbons driven from the coal by the felsite. 
 
 In Selection 1767, two and a half miles above the junction of Munna Creek with 
 the Mary River, the following strata dip at 11° to N. 30° E. :— 
 
 Ft. in. 
 Shale ie ot Re ae ne af ee 0 
 Bright bituminous Coal (Top Seam) Ay, Ae ads = 8 2 8 
 Black coaly shale aS Aa ak 
 Bright bituminous Coal with a few thin bands (Botton Seam) Bie a0 
 Black and brown shales ... ~ Ke oe Fs veh ae 3 3 
 Coal and shale mixed .., es se a a ee ae 0 
 
 In his “ Report on the Coal Deposits of West Moreton and Darling Downs,” Mr. 
 Gregory gives the following analysis of coal from “ Miva Seam, Mary River’: — 
 
 Volatile in coking ue 0 anit ai at it ae 23°6 
 Fixed carbon a wae 50h ee a Kee <6 ies 61:0 
 Ash Ae a! ae ae te + A =e ei 15°4 
 
 100°0 
 
 Coke, 76°4; Carbon in coke, 80; Ash in coke, 20. 
 
 From some expressions in his “ Report on part of Wide Bay and Burnett 
 Districts,” I infer that this Miva Coal is the same as that in Munna Creck. 
 Vv 
 
306 
 
 On Tanyalba Creek, about a mile and a half north of the last section, are two 
 
 thick seams of impure coal, as in the following sections :— Ft. in, 
 Nodular clay-ironstones and shales aa <i 
 
 Coal (very impure) : 7a 
 Sandstone and shale a oe a or wi eh ae OLED 
 Coal (impure) ere 5 9 
 Black carbonaceous ales +; et oe a et be (iO 
 Alternate bands of Coal and shale én ws 40 5 
 In Jones’ Selection, No. 1311, the fonlewine mip W. 10° S. at 40° :-— ap! 
 » sll. 
 
 Brown Sandstone ...-  ... oy oe Pes oH ‘AP fo eo mU 
 Sram I.— 
 
 Bright hard Coal = sa is ore a es Eeil 
 
 Black coaly shale ge Wis 7 eee Oe Det aoe 
 
 Bright hard Coal _... th ee sh ome dy eee 1 43 
 Fireclay _... oe 2 dae i ee ie oa cee Oe 
 Coal ... Ae 09 
 Fireclay sae be es iat ss ns a wag 3.9 
 Coal ... es ah Sn * sy A az see oe 0 6 
 Clay .. et ae oi oo vege WO ea 
 Coal ,.. st ie Bg Res nes a wre eae Ne 0 9 
 Clay’... an bu, a on PP ses = fi sa Wf 
 Coal ... oO; ate sae aes aa ae ae ae 550 07 
 Clay .. A x - a se ¥ ae G9 
 Sram oe Coal 3 6 
 Sandstone ... Wes AY — Ty a Re ses 1 0 
 Clay and black shale 3 0 
 Sram JIT.— 
 
 Coal 
 
 Clay band hah om rh an ive Ae re 
 
 Coal. -.5. oe shi aa ae nee ood ae ote 
 Shale : art oe wae ave 
 
 Grey sandstone 
 
 Seam IV.—Coal : 
 
 Sandy shale with two thin beds a Cente 
 Hard brown sandstone 
 
 Black shale 
 
 Szam V.—Coal at 5 ve 
 
 Two chains higher up the Creek, a three feet seam of coal is said to be visible in 
 a waterhole. At the northern boundary fence of the Selection (still higher up the 
 Creek), a hard bright coal-seam of good quality, three feet thick, can be seen in a 
 waterhole. It is probable that this seam is the same as No. 1 in the above section. 
 
 In Selection 1737 (Sorensen’s) is a seam of coal two and a half feet thick, with 
 sandstone above and below. 
 
 On the western slope of Mount Bopple the Coal Measures are altered by contact 
 with the mass of micaceous granite of which the western slope of the mountain consists, 
 and graphite is met within a shaft. The following are Analyses of the graphite by 
 Mr. Rands. No. 1 was a picked sample, and No. 2 was made up of the pieces of the 
 shale and bands of graphite taken from over the whole section :— 
 
 ro 
 OrOOCOrF OFF CO 
 ee 
 
 EP POPRAar & wb bd 
 
 NOveLe No, 2. 
 Carbon a tk Bc on TPA) cee 44°25 
 Moisture and volatile atten At: a a 6'3 Ato 7-00 
 Ash eae See ane see ric e See 21:0 ae 48°75 
 
 
 
 
 
 1000 100°00 
 
307 
 
 A three feet seam of coal is said to have been discovered some years ago in 
 Selection No. 90, opposite Aurora Plantation. 
 
 Two hundred yards above Selection No. 78, on Redbank Creek, is a seam of good 
 bright coal, four feet two inches in thickness. 
 
 In Selection No. 39, west of Aurora, is a seam of bright coal, thirteen inches 
 thick and nearly vertical. 
 
 AnaLysEs (Rands). 
 
 
 
 
 
 
 
 
 
 
 
 Volatile ‘a : 
 Water. Hydro. Cason Ash. oo Coke. 
 Seam in Bull’s Selection (1537)... he 7:0 86 68°4 16:0 150 | 81°4% 
 (grey) | 
 Selection 1767, Munna Creek (Top Coal) ... 6:0 22°6 49°9 21°5 1:43 71:2 
 | (grey) 
 “ay 4 (BottomCoal)} 50 | 29:0 | 485 175 153 | 660 
 (reddish 
 grey) 
 Jones’ Selection (1311) Seam I... Ss 2°5 2671 62°9 85 1°32 714. 
 (arey) 
 "a f 2 Tite ah RO) le 92-4 eh) B11 20°5 1:38 | 71:6 
 (reddish) 
 ” %» » \ Sota eee eS 30°0 39°5 16°5 zat 53'0 
 (grey) 
 Ny 3 a in waterhole 5b 28:7 b1s3 14°5 1°38 65'8 
 (grey) 
 Sorensen’s Selection (1737) ... ea 38 12:0 34:2 32°8 21-0 np 53°8 
 (white) 
 Redbank Creek, above Selection 78 ae 10:0 28:0 4.7°5 14:5 5E 62°0 
 (reddish 
 grey) 
 
 
 
 
 
 
 
 
 
 * Non-Caking. 
 
 Mr. Rands remarks that the high percentage of water and ash, as well as the 
 high specific gravity, are due to a great extent to the specimens for analysis having been 
 taken from the outcrop of the seams. 
 
 Mr. Gregory’s “ Report on the Wide Bay and Burnett Districts” contains a few 
 references to the part of the Coal Field near Bundaberg, to the north of Burrum. 
 
 An eight inch seam is seen on the south side of the Burnett District, about eight 
 miles above Bundaberg. Above the coal are eighty feet of brown sandstones and shales. 
 Borings to the depth of one hundred and forty feet below the coal showed black shales 
 and several seams of coal, but nothing workable. Several thin seams of coal are 
 exposed by Pine Creek, which falls into the Burnett three miles above Bingera. In an 
 Appendix to his “ Report on the Coal Deposits of West Moreton, &c.,’ Mr. Gregory 
 gives the following analysis of coal from Pine Creek :— 
 
 Volatile in coking... as, te et a Si ree . 3843 
 Fixed carbon a ae aa aac Saf — 6 fon OAS 
 [A sivaae Dan dee Be ats roe ee hic Koa ue 6:2 
 
 98°0 
 
 Coke, 68°7; Carbon in coke, 90°3; Ash in coke, 9°7. 
 
 OUTPUT OF THE BURRUM COAL FIELD. 
 It is only since the opening of the railway from Maryborough that the Burrum 
 Coal Field has been worked to any extent worth mentioning. During the last eight 
 years, the output has amounted to 187,761 tons, valued at £160,016. 
 

 
 308 
 
 YIELD OF BurrumM Coat FIE Lp. 
 
 1883 6,140 tons raised; value £38,780 
 1884 6.180. = » 3,550 
 1885 yt ely. » 14,950 
 1886 AW st. pc. SO ods ee » 28,189 
 1887 ae Bis er oe a. 45,527 5 oF 25,609 
 1888 56,684 ,, » 80,096 
 1889 48,267 _,, » 25,916 
 1890 58,781 f 83,2926 
 
 
 
 761 * » £160,016 
 
 The Styx Coal Field, near St. Lawrence, appears, from its fossils, to be on the 
 same horizon as the Borrum Beds, although occurring in an isolated area. Where the 
 road from Rockhampton to St. Lawrence crosses Deep Creek, one of the heads of the 
 Styx, the Coal Measures uncomformably overlie shales of the Gympie Beds. To the 
 north they are capped unconformably by the Desert Sandstone (?) at Wilangi. To the 
 east, between Wellington Creek and Bald Hills, beds of encrinital limestone occur in 
 the Gympie Beds, and to the west are the fossiliferous beds of Yatton, belonging to the 
 same series. JI am indebted for the above particulars to Professor T. W. Edgeworth 
 David, B.A., and the late Mr. James Smith. 
 
 Ata point which is described as being eighty miles from Rockhampton, and 
 twenty five from St. Lawrence by road, a shaft has been sunk to the depth of seventy 
 feet. Twoseams of coal were met with in this shaft, one said to be between sixty five 
 and seventy feet from the surface and seven feet thick, and the other between three 
 and four feet thick, but the depth is not stated. The late Mr. A. B. Lindon gave the 
 following as an Analysis of the Coal :— 
 
 Totals ate 187 
 
 
 
 Moisture = 2°2 
 Volatile hydr eahgin ace ole 
 Fixed carbon x 62°6 
 A‘s hi eee eee sevie GH) 
 
 Total . . 100°0 
 
 A sample of the coal was treated by Mr. F. Linthwaite, Locomotive Superin- 
 
 tendent of the Central Railway. 
 sample of coal has not been used on this line.” 
 
 waite is as follows :— 
 
 According to Mr. Linthwaite’s Report—“ A better 
 The Driver’s Report to Mr. Linth- 
 
 * Queensland Central Railway, 
 “ Locomotive Department, 
 “Rockhampton, July 6th, 1889. 
 
 “ Report to Locomotive Foreman, 1st July, 1889, ve Trial of Coal. 
 ‘Str,—I have the honour to report that I found this coal to be very good for steam 
 
 raising. Itis very easy to work, and very clean, making very little ashes. 
 
 In fact, I consider 
 
 it equal to any Newcastle coal that we have been supplied with. 
 
 Weight of— 
 Train 
 
 Coal 
 
 Ashes in fire-box a aac -pan . 
 
 Ashes in smoke box 
 Miles run 
 
 First Dass Second Day. 
 tons. cwt. qr. ewt. qr. lb. 
 1260 0 5 ~ 
 +4 1 0 0 
 
 vf. ay (8) BiS0R26 
 La? Ome 
 165 225 
 
 Barcaldine to Alice, 60 tons. 
 
 * Weight of train on second Bayete Saceadnenns "36 tons; to Barcaldine, 69 tons; 
 + This is the total quantity of coal used on both days. 
 
 - The run was 390 miles. In addition to the above there was the necessary shunting to 
 
 be done at the commencing and concluding of each day’s run. 
 “C. Grit, Engineman. 
 
 Rockhampton to Barcaldine, 
 1S bas 
 
 “ Average consumption, 23°030 lb. of coal to the mile. 
 thence to Alice ; in all, 390 miles.” —* Say, 23% lb. to the mile. 
 
309 
 
 Another shaft was sunk in 1890, by the Broadsound Coal Mining Company, near 
 the Waverley Creek Wharf, to the depth of ninety six feet. From ce bottom of the 
 shaft a bore was sunk, making the total depth one hundred and twenty eight fect. At 
 ninety eight feet was a coal-seam fifteen inches thick. At one hundred and) twenty feet 
 
 the following section was met with :— Ft. in, 
 Coal, very hard splint... es a ne mie ue i 3 
 Band soft grey clay a Sees: a 0 6 
 Coal, mixed splint and Ineaihinoue, 2 0 
 Band clay ake 1 4 
 Coal , 1 8 
 
 Professor T. W. E. Aiessts regards ‘irs eet seam at the bottom of the bore as lying 
 about two hundred and eighty feet above the lowest seam in the basin. 
 VERTICAL SECTION OF THE BROADSOUND COAL BASIN OR STYX ee FIELD. 
 
 in. 
 
 Stiff dark grey clay ee ie ae i e: Se 20 0 
 | ueiaherniee 
 
 Magnesites with fine-grained yellowish-grey sandstone (approximate) 100 0 
 Unconformity. 
 
 Shales with lenticular bands of ironstone or ue si ok 0 4 
 
 Strata unknown. Section of them can be easily obtained by 
 trenching in the salt pans, and the outcrops of any seams of 
 
 | coal which may exist in them could be proved in the same 
 manner : ak 61,000" 0 
 
 ee with red dial: econ oeeaehions eonerctone with thin 
 beds of sandstone and limonite septaria ... ae ey a - 00 0 
 a carbonaceous sandstone... ve ete ae an 
 Argillaceous sandstone with bands of Saeline: fee bas Bee We GW 
 Tough calcareous sandstone, fine-grained, lenticular ... vas ase 2 0 
 Dark mudstone _... Si, aii i = xs ae sete EUR TY 
 Hard grey sandstone ee Mer * oF, met vai ae 2.0 
 Dark grey sandstone — oa ase <s asa a Le ee) RT) 
 Hard grey sandstone shi re ea nae ee ae see 2 0 
 Hard sandy ironstone _... ee ae Sa OR a +5 0 4 
 e] Massive clayey sandstone 55 sa BS, hie Slee ee SW) 
 Mudstone ... a a ns mak 365 oe as a BELO ED) 
 ae Massive eardstcna af Bee ee rs; “a ite age A 
 4 Mudstone ... . ae ie me “ft eae oe 
 ! Thin-bedded, very ale sandstone. ee ba e: ss caeod a. U 
 Clayey sandstone ..., : "a re re es en ew 
 Sandstone, with ironstone Candee we 4 Petes OU 
 Massive soft carbonaceous sandstone with enon bends eo | O 
 
 Shaly sandy ironstone, with white fireclay and a band of sandy car- 
 | bonaceous ironstone full of fossil plants (about) ‘ UL 
 ( Whitish-grey, and rusty sandy shales with band of fe toce as, 0 yah 
 
 : Crumbling brown mudstone, grey and rusty sandy shales, and 
 crumbling mudstone : ts as ca BO) 0 
 Crumbling sandstone, with caicareous Sona eHone at it as 8 O 
 Soft sandy shales, crumbling in weathering ... bs ie ee et. 0 
 Sandy shales, with forruginons concretions... ae ae Sa 8 0 
 Lenticular argillaceous limestone ee ie oe. 6 
 
 | Soft crumbling mudstone and sandy shales, with dark-br own 1 maacly 
 f shales, and thin bands of sandstone weathering rusty... ee WSO a) 
 
 
 
 
 
 1. Section of strata in first anticline 480 feet. 
 2. Section of strata seen in second anticline, 260 feet. 
 3. These strata can be tested most economically by trenching. 
 
310 
 VERTICAL SECTION OF THE BROADSOUND COAL BASIN OR STYX COAL FIELD— 
 
 continued. 
 
 Aes ok clayey, carbonaceous sandstone AG ~ ie OS 
 Coal . os his ne i sf yas oof sien cee 0 
 Coal . ot - ce O 
 rn | Nodules of clay fronetone: 1 
 ’ | Coal and shale mixed sas ais ote ead ae oP or if 
 Nodules of clay ironstone aa 2 se a ae mei 0 
 Shaly sandstone, gritty in upper 5 fect - ee 
 Hard greenish-grey calcareous sandstone, with praing = eoal oven BEL 
 (Strata unknown. No section obtainable—coal-seams probably 
 occur in these strata (very approximate) . re . 1,85 
 Sandstone rather coarse, with bean-shaped concretions of Timontie? 
 there is a thinly bedded coal-seam here (?) probably the one now 
 struck at No. 1 shaft, Newport... a6 are 20 O 
 Grey sandy shale with bands of clay ironstone from } inch to 3 
 | inches thick (approximate) ... - se ore 5S: ve de 
 | Coal-seam hereabouts (?). Mainseam (?).  ... ARE 
 
 o 
 
 
 
 Grey sandy shales with bands of clay ironstone 5 inch to 3 inches 
 
 thick ... ae er see ax a ne 0 3 
 Whitish-grey calcareous élay shale - ay sas Pe 
 Sandstone fairly hard, fine-grained, flaggy, carbonaceous, in upper 
 
 5. 
 
 
 
 part hard calcareous ees re ae sor Rel 
 Clayey ironstone with abundant fossil plants Sai aes os sae 0 6 
 Grey sandy caleareous clay shale (approximate) a one DU 
 Band of clay ironstone with fossil plants ae ns ss oh O 6 
 (| Fine sandstone (very approximate) .. f 10,0 
 
 Massive glistening hard sandstone, eeryinltta Hawleabury Sand- 
 stone of New South Wales, contains casts of plants, and at 
 | base of bed, where it passes into a fine conglomerate, as near 
 ‘the Pilot Station, St. Lawrence, it shows casts of Spirifers and 
 | Martinia subradiata, a shell in New South Wales especially 
 d characteristic of the Permo-Carboniferous Formation in which 
 occur the valuable Greta Coal Measures. Part, therefore, of 
 this bed, and portion of the underlying strata, probably are of 
 Permo-Carboniferous age, and may contain the Greta CoalSeams 50 0 
 Hard shales, dark grey and light grey, with thin bands of ironstone 
 at top of series, and beds of cherty shales with <Archa@o- 
 Ma calamites (?) 
 Coarse pebble conglomerate ie bree in tne rade of the posccn 
 Unconformity. 
 
 6. 
 
 Limestone. 
 Limestone. 
 Dark gray argillaceous felsites. 
 Quartz felsites. 
 4, J. B. Christian and Coy., Shaft, 152 feet. 
 5. These strata can be prospected by means of a number of shallow shafts. 
 6. Strata usually associated with the Greta Coal Measures. 
 Since the above was written Mr. W. H. Rands has completed a survey and made 
 a report on the Styx Coal Field. The report contains a mass of valuable information 
 regarding the coal-seams, but throws little light on the age of the measures. Mr. Rands 
 says: ‘There is no evidence to show whether they (the Coal Measures) are the equivalents 
 of the Ipswich or the Burrum Beds. All that can be said with certainty is that they are 
 Mesozoic. They are older than the Upper Cretaceous Desert Sandstone, by which they 
 
dll 
 
 are overlaid unconformably, and newer than the Permo-Carboniferous rocks, in a depres- 
 sion of which they have been deposited, and on which they are resting unconformably. 
 I understand from Professor Edgeworth David, who spent some time in this district 
 examining these beds, that Zeniopteris was met with in Mr. Christian’s shaft in Foyle 
 Park. I also found a few indistinct leaf-markings in shales in Foyle Park, but, with 
 these exceptions, I believe no fossils have yet beenfound. . . . Evidence of contem- 
 poraneous volcanic action is met with in Shaft No. 5, Waverley Creek, where fifty-seven 
 and a half feet of tufaceous sandstone, containing white porphyritic particles, were 
 passed through.” 
 
 Mr. Rands estimates the thickness of the Coal Measure strata, in the neighbour- 
 hood of Tooloombah and Deep Creek, at about five thousand feet. 
 
 It may be remarked that the paucity of fossils in the Styx Coal Measures is a 
 characteristic feature of the Burrum Coal Field also—whatever may be the value of such 
 purely negative evidence. On the other hand, the presence of contemporaneous igneous 
 rocks in the Styx Coal Measures is a point which the latter have in common with the 
 Ipswich Coal Measures and not with those of Burrum, so far asis known. 
 
 LIST OF FOSSILS OF THE BURRUM BEDS, WITH THEIR SYSTEMATIC POSITIONS. 
 
 Kingdom—PrLantH. 
 Section—CRYPTOGAMIA. 
 Class—ACOTYLEDONES. 
 Order—FILiczs. 
 Family—SPHENOPTERIDE. 
 Genus—SPHENOPTERIS, Brongniart. 
 Sphenopteris flabellifolia, Ten. Woods. 
 Loc. ‘ Burnett River, half-way between Bundaberg and Five Coal Seams.” 
 Sphenopteris flabellifolia, var. erecta, Ten. Woods. 
 Loc. As above; and “ Burrum Coal Field.” 
 
 Genus—TRICHOMANITES, Goeppert. 
 Trichomanites laxum, Ten. Woods. 
 Loc. Burrum. Occurs also at Rosewood, near Ipswich. 
 
 Family—PECOPTERID. 
 Genus—ALETHOPTERIS, Sternberg. 
 Alethopteris australis, Morris. 
 Loc. ‘ Burrum Coal Field.” Occurs also at Stewart’s Creek, Rockhampton, and in the 
 Ipswich Formation. 
 
 Family-—NEUROPTERIDE. 
 Genus—THINNFELDIA, Ettingshausen. 
 Thinnfeldia media, Ten. Woods. ? 
 Loe. Burrum Coal Field, near Maryborough. Occurs also in the Ipswich Formation. 
 
 Family—TZNIOPTERIDE. 
 Genus—T2£NI0PTERIS, Brongniart, 1828. 
 Teniopteris (? Angiopteridium) Daintreei, McCoy. 
 Loc. Styx Coal Field (Burrum Beds). Occurs also in the Ipswich Beds. 
 Section— PHANEROGAMIA. 
 Class—DiIcoTyLEDONEs. 
 Order—CYCADACER. 
 Family—ZAMIEx. 
 Genus—Popozamitgs, F. Braun. 
 Podozamites Kidstoni, Eth. fil. 
 Loc. Burrum Coal Field, near Maryborough. 
 Podozamites, sp. ind., Pl. 18, f. 4. 
 Loe. Burrum Coal Field, above the Bridge Scam. 
 
312 
 
 Genus—OTozAmiTEs, F. Braun. 
 Otozamites,? sp ind., Pl. 17, £. 8. 
 Loc. Burrum Coal Field, above the Bridge Seam. 
 
 Order—ConIFER®. 
 Family-TAxacEz. 
 Genus—BArERA, F. Braun. 
 Baiera bidens, Ten. Woods. 
 Loc. Burnett River. 
 
 Kingdom—ANIMALIA. 
 Sub-Kingdom—MOo .tvsoa. 
 Section— MOLiLUSOA VERA. 
 Class—PELECYPODA. 
 Order—VENEBRACEA. 
 Family—CYRENIDE. 
 Genus—CorbicuLa, Miihlfeldt. 
 Corbicula burrumensis, Eth. fil., Pl. 34, figs. 9 and 10. 
 Loc. Queensland Co.’s Coal Mine, Burrum. 
 
 Order —PHOLADACEA. 
 Family —GASTROCHANIDE. 
 Genus—RoceLuaRtA, Blainville. 
 Rocellaria terra-reging, Eth. fil. 
 Loc. Queensland Co.’s Coal Mine, Burrum. 
 
 SYNOPSIS. 
 
 OccoURRING IN Burrum Formation. 
 Sphenopteris flabellifolia, T.W. 
 0 sy var. erecta, T.W. 
 * Trichomanites lacum, T.W. 
 * Thinnfeldia media, T.W.? 
 * Teniopteris Daintieei, McCoy (Styx River). 
 * Alethopteris australis, Morr. 
 Podozamites Kidstoni, Eth. fil. (sp. nov.) 
 c sp. ind., Pl 18, fig. 4. 
 Otozamites,? sp. ind., Pl. 17, fig. 8. 
 Baiera bidens, T.W. 
 Corbicula burrumensis, Eth. fil. (sp. nov.) 
 Rocellaria terra-reging, Eth. fil. (sp. nov.) 
 * Also iu Ipswich Formation, including Stewart ’s Creek (Rockhampton) Beds. 
 Of the twelve species above named, four are common to the Ipswich Formation, and the remaining 
 eight are peculiar to the Burrum Formation. 
 
 It will be seen from the preceding list that, with the exception of the genus 
 Sphenopteris, the Burrum Formation has nothing in common with the Permo- 
 Carboniferous System. 
 
 On the other hand, as four out of ten plants are specifically identical with 
 plants occurring in the Ipswich Formation, the connection between the two formations 
 must be a close one. When my Geological Map was published in 1886, I inclined to 
 regard the ‘‘ Burrum Beds” as Triassic and the “ Ipswich Beds” as Jurassic, but, in 
 view of the more complete evidence now available, it seems reasonable to regard them 
 as subdivisions of a single period—the Trias-Jura. The Burrum Beds, therefore, are 
 provisionally classed as Lower Trias-Jura. 
 
 J. 
 Note 'ro PAGE 7.—The heading of the paragraph occurring after the Yield of Herberton Tin Field 
 should read ‘*‘ Kangaroo Hills and Running River Tin and Silver Fields.” The Running Creck referred to 
 in the next paragraph is in the Star River District. 
 
 
 
 ‘ 
 eet te i a . 
 
CHAPTER XXIV. 
 
 THE ORGANIC REMAINS OF THE TRIAS-JURA SYSTEM, 
 
 Witn Descriprions oF THE SPECIES OCCURRING IN THE BurruM ForRMATION 
 (Lower Trras-JURA). 
 
 In this System are comprised such fossiliferous strata as lie, so far as their 
 position can be ascertained, between those horizons representing the uppermost Fresh- 
 water Coal Measures of the Bowen River Coal Field, and the Rolling Downs Formation. 
 
 This Series is of the utmost importance, because it contains the chief workable 
 coal-seams in Queensland, or at least the principal seams at present worked. The 
 organic remains are principally those of plants, with a strong Mesozoic facies, and 
 oscillating, in all probability, between the Trias and Upper Oolite in age. They have 
 been studied by Messrs. Carruthers and Feistmantel, and the late Rev. J. E. Tenison 
 Woods. The last named, in his “ Fossil Flora of the Coal Deposits of Australia,’’ 
 has endeavoured to assign many of these plants to horizons corresponding with those of 
 their nearest allies of Europe and elsewhere, and in this way has accounted for the 
 presence in Queensland of the Trias ? Rhetic or Lower Lias, Upper Lias, and Jurassic. 
 But our knowledge of these plant beds is too young at present for such minute sub- 
 division, and we know far too little of the association of the species one with the other, 
 and the similar relation of their respective matrices, to assign minute geological horizons, 
 on the chance of a mere guess, or hasty generalisation, turning out correct. 
 
 The principal deposits yielding Mesozoic plants in Queensland are :— 
 
 Ipswich Coat Measures at— 
 Redbank, near Mount Esk, Brisbane River. 
 Cressbrook and Colinton, Brisbane River. 
 Bundanba Colliery, Ipswich. 
 Tivoli Colliery, Ipswich. 
 Walloon Colliery, Ipswich. 
 Rosewood (Southern and Western Railway). 
 Peak Mountain, near Fassifern, twenty miles from Ipswich. 
 Talgai, near Warwick. 
 Darling Downs, near Toowoomba. 
 Stewart’s Creek, near Stanwell. 
 Wycarbah (Rosewood), near Rockhampton. 
 Burrum Coat Mreasurrs— 
 Burnett River Beds. 
 
 The Organic Remains from Stewart’s Creek and Wycarbah are grouped with those 
 of the Ipswich Formation. 
 
 In a Paper “On Various Deposits of Fossil Plants in Queensland,’’* the Rev. 
 J. H. Tenison Woods gives the locality of Peak Mountain, near Fassifern, and quotes 
 from it plants like Rhacopteris. Strange to say, I do not find this place mentioned in 
 his more extended Memoir on the Coal Plants. He remarks that if the plants found 
 there belong to Rhacopteris their occurrence “would indicate a much lower horizon 
 than any beds hitherto found in Queensland.’ On looking over Mr, Wood’s Collection, 
 
 
 
 * Proc, Linn. Soc. N. S. Wales, vii., Pt. 1, pp. 95-98. 
 
314 
 
 now in the Macleay Museum, Sydney University, I found several well-marked and well- 
 preserved examples of Alethopteris australis, Morris, sp., and Yeniopteris. This will 
 naturally assign, instead of a Paleozoic age, one quite in accordance with the other 
 beds of the Ipswich Basin. Many other deposits containing Mesozoic plants exist in 
 Queensland, but it is not deemed necessary to mention them here. 
 
 Glossopteris has, on several occasions, been quoted as occurring with other Mesozoic 
 plants in Queensland. I can only say, however, that during an experience extending 
 over ten years, not one single instance of Glossopteris associated with a flora repre- 
 senting beds higher than the Freshwater Series of the Bowen River Coal Field has come 
 under my notice. This sharply defined line, so far as I know, appears to hold good 
 equally well for New South Wales. There is no reliable record of this genus being 
 found at any horizon higher than the Upper, or Newcastle Coal Measures in the latter 
 Province. Allied genera, such as Sagenopteris, do occur, but not the true Glossopteris, and 
 it is probable that in cases, such as above referred to, the one has been mistaken for the 
 other.* 
 
 DESCRIPTIONS OF THE SPECIES OCCURRING IN THE BURRUM FORMATION 
 (LOWER TRIAS-JURA). 
 
 Kingdom—PLANTA, 
 Section—CRYPTOGAMIA. 
 Class—ACOTYLEDONES. 
 Order—FILICES. 
 Family—S PH ENOPTERID®. 
 
 Genus—SPHENOPTERIS, Brongniart, 1828. 
 (Prod. Hist. Vég. Foss., p. 50.) 
 
 SPHENOPTERIS FLABELLIFOLIA, Ten. Woods. 
 Sphenopteris (Aneimioides) flabellifolia, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., Pt. 1, p. 94. 
 
 Sp. Char. .Frond delicate, small bipinnate, rachis terete, somewhat thick; pinns 
 oblong, cuneate, contracted at the base to a delicate petiole, lower edge entire, upper 
 divided into linear cuneate lobes of varying width, the edges straight or rounded, some 
 of the pinnez much elongated, costa inconspicuous, veins fine, close, numerous, straight, 
 radiating. (Zen. Woods.) 
 
 Obs. This species is said by its Author to possess a strong resemblance to 
 Archeopteris. The type specimen reminds me of a small species of Dawson’s genus 
 Aneimites. 
 
 Loc. Burnett River, half way between Bundaberg and Five Coal Seams (Rev. 
 J. E. T. Woods)—Blue shale. 
 
 SPHENOPTERIS FLABELLIFOLIA, var. ERECTA, Ten. Woods. 
 
 Sphenopteris (Aneimioides) flabellifolia, var. erecta, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1888, viii. 
 Puede PaeGae ta zeke 2s 
 
 Obs. Of smaller size, and regularly pinnate, the pinnw lobed or segmented 
 symmetrically at both sides. Although differing from the species proper, the venation 
 
 
 
 * Since the above was written, a plant which I have satisfied myself is a true Glossopteris has been 
 found by Mr. W. H. Rands, near Pentland, on the Nortkern Railway, in strata which my Colleague has 
 ascertained to lie nec ntomiatly on the ‘‘ Rolling Downs Formation,” and which, therefore, he believes 
 to be part of the Desert Sandstone. See Chapters on the Desert Sandstone. (R. EZ. Junr.) 
 
 
 
315 
 
 and general shape of the lobes is said to be the same. As this fern occurs intimately 
 
 mixed with the preceding on the same slab, it must be retained as a variety, although 
 
 individual specimens here and there differ widely. It is not unlike an Hremopteris. 
 Loc. With the preceding, and in the Burrum Coal Field (W.H. Rands). 
 
 Genus—TRICHOMANITES, Goeppert, 1836. 
 (Syst. Fil. Foss., p. 174.)* 
 TRICHOMANITES LAxuM, Ten. Woods? PI. 18, fig. 9. 
 Trichomanides laxcum, Ten. Woods, Proc. R. Soc. N. 8. Wales, 1883, viii., Pt. 1, p. 95, t. 10, f. 2. 
 
 Sp. Char. Rhizome creeping, long, slender, sending up at distant irregular 
 intervals delicate membranaceous pinnate fronds; pinne emerging at an acute angle, 
 linear, or cuneate, bifurcating with one simple free vein to each lobe. (Zen. Woods.) 
 
 Obs. T. laxum is said to be distinguished from 7. elongata, Carruthers, sp., by 
 being much smaller, and consisting “of short pinnate fronds proceeding at irregular 
 intervals from the slender creeping rhizome.” 
 
 Mr. R. Kidston believed he could recognise this amongst Mr. Rands’ Collection 
 of plants from the Burrum Coal Field. He remarks as follows :—‘‘ This fossil shows 
 a fragment of a very graceful species. The pinnules are divided into a number of 
 simple, or bifid-linear, acute segments. The characters of Z. lawum are simply 
 unintelligible. If Mr. Tenison Woods supposed his figure to represent a rhizome, as 
 I am led to think from his description, there appears to be a mistake in the interpre- 
 tation of the fossil, which more probably shows part of a compound frond.” 
 
 Loc. Burrum (W. H. Rands). Occurs also at Rosewood, near Ipswich. 
 
 Family—NEUROPTERID. 
 
 Genus —THINNFELDIA, Ettingshausen, 1852. 
 (Abhand], K. K. Geol. Reichsanstalt, i., Abth. 3, No. 3, p. 1.) 
 
 THINNFELDIA MEDIA, Ten. Woods, Pl. 17, fig. 2, Pl. 18, fig. 10. 
 (Compare Pl. 17, f. 7.) 
 
 Thinnfeldia media, Ten. Woods, Proc. Linn. Soc. N.S.-Wales, 1883, viii., Pt. 1, p. 102, t 6, f. 1. 
 (Compare Thinnfeldia indica, Feistmantel, Pal. Indica (Gondwana Flora), 1877, i., Pt. 2, t. 39, f. 1, 1d, 
 t. 46, f. 1-2 a.) 
 
 Sp. Char. Frond bipinnate? pinnee quite close, nearly opposite, broadly lanceo- 
 late, broadly obtuse ; the lower ones shorter, attached by the whole of the base where 
 it is only very slightly constricted; veins only faintly visible, but there are traces of a 
 costa in nearly all the pinnules, which is evanescent ; rachis very thick. (Zen. Woods.) 
 
 Obs. These characters were assigned by the Rev. Mr. Woods to a plant from 
 the Hawkesbury Sandstone of Dubbo, which he compared to Thinnfeldia indica, Feist- 
 mantel. “It bears some resemblance to Z indica, Feistmantel, and more to 7. 
 decurrens, Schenk.” | 
 
 With specimens of the Dubbo plant I am not acquainted, but in referring 
 the Queensland ferns (PI. 17, fig. 2, and PI. 18, fig. 10) to Z. media I am simply relying 
 on Woods’ description, and his reference to 7. indica, to which the figures undoubtedly 
 havea strong resemblance. It must, however, be acknowledged that such a point as 
 “veins only faintly visible’? does not wholly agree with our specimens; but on the 
 other hand, “attached by the whole base,’ “traces of a costa,” and “ rachis very 
 
 
 
 * Die fossilien Farrnkriuter (Wova Acta. Acad. Leopol. Carol. Curiosorum, Bd. xvii., Suppl.) 
 
516 
 
 thick,’’ are features plainly visible in the Queensland specimens. In the example from 
 the Burrum (Pl. 17, fig. 2) the venation is indistinct, and we have only the form of the 
 leaflet to guide us, and this is unmistakably that of Z indica. In the subject of 
 Pl. 18, fig. 10, the venation is very strongly marked, the peculiar right-angled 
 deflection and bifureation, so characteristic of Zhinnfeldia, being present ; and, finally, 
 there are traces of a by no means weak costa. Here again we observe a marked 
 resemblance in the outline of the pinnules to those of Z. indica, particularly Pl. 39, 
 fig. 1, of the reference above cited. 
 
 I may, perhaps, be again allowed to refer to Pl. 17, fig. 7, representing a specimen 
 which seems to oscillate between the type species and this form, or perhaps one of the 
 varieties of the former. It is very like the type of Woods’ 7. media in the Macleay 
 Museum, Sydney University. 
 
 Mr. G. Sweet has obtained a bifureating frond, seven inches long, with a large 
 number of pinnules zz s¢tu, which are either long and curved, lanceolate, diminishing to 
 a fine distal point, or short, obtuse, and bluntly rounded, both on opposite and the 
 same sides of the rachis. There is a decided false midrib to the pinnules, which disap- 
 pears before reaching their apices. The rachis, below the bifurcation, is nearly three 
 and a half inches long, and striate, with pinnules on each side. The form of the 
 pinnules is precisely that of Feistmantel’s Pl. 46, f. 1, and the habit that of his Pl. 39, 
 f.1. The specimen greatly confirms me in the belief that Thinnfeldia media and T. indica 
 are very near, if not identical. 
 
 Loc. Burrum Coal Field, near Nance Pl. 17, fig. 2 (W._H. Rands). 
 Occurs also in the Ipswich Beds. 
 
 Family—PECOPTERIDZ. 
 
 Genus—ALETHOPTERIS, Sternberg, 1826. 
 (Flora der Vorwelt, Heft 4, p. xxi.) 
 
 ALETHOPTERIS AUSTRALIS, Morris, Pl. 16, fig. 1. 
 Pecopteris australis, Morris in Strzelecki’s Phys. Descrip. N. S. Wales, &c., 1845, p. 248, t. 7, f. 1 and 2. 
 Alethopteris australis, Schimper, Traite Pal. Vég. 1869, i., p. 569. 
 Pecopteris australis, McCoy, Geol. Survey Vict., Decade ii., 1875, p. 16, t. 14, f. 3. 
 Alcthopteris australis, Feistmantel, Pal. Indica (Gondwana Flora), 1876, ii., No. 1, p. 24. 
 * (Pecopteris) australis, Feistmantel, Palaeontographica, 1879, Supl., Bd. iii., lief 3, heft 2, p. 109, 
 t. 14, f. 1 and 1a; heft 3, p. ,169, t. 12, f. 5, 5a. 
 os australis (Asplenium Whitbyense, Heer), Feistmantel, Ral. Indica (Gondwana Flora), 1881, iii., 
 No. 3; p. 79: : 
 op », Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. 1, p. 111. 
 
 Obs. This fern has been so adequately described by Morris, Feistmantel, McCoy, 
 and Woods, that it is not necessary to repeat the description here. 
 
 Several very fine examples have been collected in the Ipswich Basin; one of these, 
 from Bundanba, is a portion of a frond, eight inches long, and shows a spread of the 
 pinne equal to seven inches. In the former space there are portions of four pinne, three 
 attached to the rachis. This will afford some idea of the size to which it attained, two 
 of them being respectively four and five inches long. The frond, as described by the late 
 Rey. J. E. Tenison Woods, is bipinnate, and the pinne alternate and oblique. In the 
 Bundanba specimens the secondary veins of the pinnules undoubtedly fork twice, as 
 in Morris’s original examples * from the Jerusalem Basin, Tasmania. The margins of 
 the pinnules are also serrate ; but, on the other hand, specimens from Gray’s Seam, 
 Ipswich, present these entire, and the veinlets only bifurcate once. The occurrence of 
 both varieties in this Coal Basin is very interesting. The rachis is highly corrugated. 
 
 * Strzelecki’s Phys. Descrip. N.S. Wales, &c., 1845, t. 7, f. 2a. 
 
 
 
317 
 
 In his earlier writings Dr. Feistmantel followed Schimper in placing this fern 
 very near to Alethopteris whitbyense,* but latterly the same Author has united it to the 
 British fern, following Heer, referring both to the genius Aspleniwm.f On the other 
 hand, McCoy cites A. scarburgensis, Bean, also from Yorkshire Oolites, as its nearest 
 ally. In my opinion the fern figured from New Zealand, by Unger is our above species. 
 The growth is exact, and the once and twice bifureation is present. 
 
 Mr. R. M. Johnston has described § a fern under the name of Alethopteris 
 serratifolia, separating it from dA. australis on account of the serrated edges, of 
 undulating margin of the pinnules. This is unfortunate, because Morris, in his original 
 description, described || these as “either sinuous or entire, according to the position of 
 the frond.” It will be necessary, therefore, to regard his specific name as a synonym 
 of the older one. The Survey Collection contains examples of A. australis with serrate- 
 edged pinnules from Ebbw Vale Colliery and other localities in the Ipswich Basin. 
 
 Loc. Burrum Coal Field (W. H. Rands). Occurs also at Ipswich and Stewart’s 
 Creek, Rockhampton (Ipswich Beds). 
 
 Family—TZNIOPTERIDEA. 
 
 Genus—T4AANIOPTERIS, Brongniart, 1828.J 
 (Prod. Hist. Vég. Foss., p. 61.) 
 
 Tm@NIOPTERIS (? ANGIOPTERIDIUM) DaintreeEr, McCoy. 
 Obs. For description of the species see Ipswich Beds. 
 Loc. Styx Coal Field (? Burrum Beds). Occurs also in the Ipswich Beds. 
 
 Section—PHANEROGAMIA. 
 Class— DICOTYLEDONES. 
 
 Order—CYCADACESR. 
 Family—ZAMIEZ. 
 Genus—PODOZAMITES, F. Braun. 
 
 (Miinster’s Beitr. zur Petrefactenkunde, vi., p. 36.)** 
 Popozamitres Krpsront, sp. nov., Pl. 18, fig. 6. 
 
 Sp. Char. Pinne elongate, narrow; pinnules of variable size and length, distant 
 from one another, alternate, and disposed at an acute angle to the rachis; they are 
 either short, somewhat oblong club-shaped, broad, and very blunt at their apices, or 
 narrower and rather transversely elongated, abruptly attenuated or constricted at the 
 base to an articulation with the rachis. Veins numerous, close, apparently simple, and 
 more or less following the outline of the pinnules. Rachis striated and decreasing in 
 size slowly. 
 
 Obs. This rather elegant plant shows a stem four anda half inches long, and 
 aboutthree millimetres wide at its lowerextremity. On the right hand side are shown the 
 more or less perfect remains of seven pinnules, and on the other better preserved 
 
 * Pal. Indica (Gondwana Flora), 1876, ii., Pt. 1, p. 24. 
 
 + Ibid., 1881, iii., No. 3, p. 79. 
 
 + Reise Osterr. Fregatte Novara, 1857-59, Geol. Theil., Bd. i, 2 abth., 1865, p. 5, t. 2, f. 1 and 2, 
 § Geol. Tasmania, t. 23, f. 1. 
 
 || Strzelecki’s Phys. Descrip. N. 8. Wales, &c., 1845, p. 248. 
 
 | Restricted—Schimper, Traité Pal. Vég., 1869. i., p. 600. 
 
 ** Fide Zigno, Flora Foss. Formationis Ool., ii., p. 118. 
 
318 
 
 portions of five leaflets. They vary much in form and size, most of those on the right 
 side being oblong, and with obtuse apices, whilst those on the other are much more 
 elongate in proportion to their breadth. The pinnules seem to have been coriaceous, 
 and the veins are numerous, fine, and parallel. The average length of the shorter leaflets 
 is under an inch, the others reaching as much as one and a quarter inches, and imperfect. 
 
 The only fossil plant, with which I am acquainted, bearing any resemblance to 
 this is the Zamites Meneghini, Zigno,* from the Italian Oolite rocks. 
 
 Loc. Burrum Coal Field, near Maryborough (W. H. Rands). 
 
 PoDOZAMITES, sp. ind. 
 
 Obs. Several fragments, probably referable to this genus, are in my Colleague’s 
 Collection, but as the naming of mere portions of leaves, unless exceedingly well marked, 
 leads to no good end, I shall content myself by calling attention to the figures, hoping 
 that more complete specimens may eventually be discovered. 
 
 Pl. 18, f.4. Three nearly equidistant pinnules are here represented, bearing 
 five sub-parallel veins, and terminating in a sub-acute apex. The general appearance 
 of these leaves, and the bi-convex edges, giving rise to a rather transversely elongated 
 ellipsoidal figure, seem to indicate the above genus. The form of the leaflet appears to 
 be quite distinct from that of P. lanceolatus, L. and H. 
 
 Loc. Burrum, above the Bridge Seam (Hon. W. Walsh). 
 
 Genus—OTOZAMITES, F. Braun. 
 (Miinster’s Beitr. zur Petrefactenkunde, vi., p. 36.) 
 OrozaMiTEs, ? sp. ind., Pl. 17, fig. 8. 
 Obs. This fragment would appear to indicate a species of Otozamites, differ- 
 ing from O. Mandeslohi, in its much larger, fuller, and more pyriform pinnules. A 
 larger pinnule lying near the figured example has an excavate base, which heightens 
 the resemblance to this genus. The veins were probably distinct and well.marked, and 
 under twenty innumber. It may be compared to Otozamites Beanii, Lindley and Hutton,+ 
 from the Yorkshire Oolites, or O. Canosse, Zigno,t from beds of similar age in Italy. 
 Loc. Burrum, above Bridge Seam (Hon. W. Walsh). 
 
 Order—CONIFERE. 
 Obs. Vide Observations on our knowledge of the Australian fossil Conifers 
 under the head ‘‘ Ipswich Formation.” 
 Family—TAXACEZ. 
 
 . Genus—BAIERA, F. Braun, 1844. 
 
 (Miinster’s Beitr. zur Petrefactenkunde, vi., p. 21.)§ 
 
 BarERA BIDENS, Ten. Woods. 
 Jeanpaulia bidens, Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, vili., Pt. 1, p. 182, t. 4, f. 3. 
 Sp. Char. Frond broadly flabellate, segments somewhat short, often becoming 
 broader towards the apex, and ending in a short wide bifurcation, or in a curved falcate, 
 
 acute, or acuminate point; veins not conspicuous, six to ten, parallel, not branching 
 (Ten. Woods). 
 
 * Flora Foss. Formationis Ool., ii., p. 33, t. 31, f. 4a. 
 
 + Cyclopteris, Lindley and Hutton, Foss. Flora i, t. 44. Otozamites, Phillips, Ill. Geol. York., 3rd 
 edit., 1875, Pt. 1, p. 220, lign. 45. 
 
 + Flora Foss. Formationis Ool., ii., p. 95, t. 37, f. 3. 
 
 § Beitriige zur Urgeschichte der Pflanzen, Abth. 1, in Miinster’s Beitriige, Heft vi., p. 21, fide Saporta 
 (Pal. Frang, Plantes jurassiques, 1873, i., p. 460)—Bronn (Index Pal., i., p. 145) gives Braun’s reference as 
 “Flora,” 1841, p. 33. 2 
 
 
 
 
 
 
 
319 
 
 Obs. The Rey. Author of this species placed it in the Ophioglossacez, under the 
 name of Jeanpaulia, following Schimper ; but [ prefer to adopt the more recent views of 
 Dr. A. Schenk. 
 
 Mr. Woods remarks that his species differs from the European Rhetic 
 B. Minsteriana, in the brevity, widening, and bifurcation of the segments. 
 
 Loe. CoalSeam of the Burnett River, Burnett District, Wide Bay (Rev. J. E. T. 
 Woods)—Macleay Museum, University of Sydney. 
 
 Kingdom—ANIMALIA. 
 Sub-Kingdom—MOLLUSCA, 
 Section—MOLLUSCA VERA. 
 Class—PELECYPODA. 
 Order—VENERACEA. 
 Family—CY RENID. 
 
 Genus—CORBICULA, Mihlfeldt, 1811. 
 (Berliner Mag., v., p. 56.) 
 
 CoRBICULA BURRUMENSIS, sp. nov., Pl. 34, figs. 9 and 10. 
 
 Sp. Char. Shell ovate, sub-trigonal, length and height nearly equal, but the 
 former rather the greater, tumid, thick and strong. Anterior and posterior margins 
 rounded, the former the more broadly so of the two. Hinge-line, or cardinal margin 
 much arched, especially on the posterior side, but the anterior more abruptly so. 
 Ventral margin regularly and evenly rounded. Posterior end, when the valves are in 
 apposition, wide and broad, giving rise to a rounded posterior slope on each valve. 
 Concentric lines of growth strong and well marked, the surface being in addition much 
 wrinkled. : 
 
 Obs. I believe this is the first recognition of this genus in Australian Secondary 
 beds. The species presents a close resemblance to C. cytheriformis, Meek, from the 
 Bad Lands of the Judith River, Upper Missouri, so much so that the above diagnosis has 
 been worded so as to express the difference between them. The Australian species is, 
 however, apparently wider in proportion to its height, and the beaks more anteriorly 
 recurved. As well as this, the shell probably possessed a more expressed posterior 
 slope in each valve. 
 
 C. burrumensis attained a fairly large size. The discovery of Mollusca in the 
 Burrum Coal Series is of importance, for only plant remains have hitherto been recorded. 
 
 Loc. Queensland Coal Co’s. Mine, Burrum (W. H. Rands). 
 
 Order—PHOLADACEA. 
 Family—GASTROCH A NIDA. 
 
 Genus—ROCELLARIA (Fleuriau de Bellevue), Blainville, 1828. 
 
 Gastrochena, Lamarck (Spengler partim), Hist. Anim. Sans Vertéb., 1818, v., p. 446. 
 Rocellaria (¥. de B.) Blainville, Dict. Sc. Nat., 1828, lvii., p. 244. 
 
 ROcELLARIA TERRA-REGINA, sp. nov., Pl. 28, figs. 13 and 14. 
 
 Sp. Char. Valves unknown; tube elongately pyriform, tapering rapidly ; anterior 
 end rounded, inflated, and somewhat flattened at the minor termination of the tube, 
 

 
 320 
 
 becoming gradually narrower towards the posterior end, which appears to be oval; 
 surface apparently obliquely striated at the anterior end, but concentrically grooved on 
 the posterior. ) 
 Obs. The Gastrochenide would appear to be a more fitting resting place for 
 this peculiar fossil than the Teridine, to which I at first supposed it to belong. The 
 fossils appear to be crypt-like tubes quite closed at the anterior end, without any trace 
 of distinct valves, such as would be apparent if it related to Teredo or its allies. 
 . The specimens closely resemble a Rocellaria figured by Stoliczka* from the 
 Arrialoor Group, but without name, but they possess a proportionately larger tube and 
 taper much more rapidly. 
 Loe. Queensland Coal Co.’s Mine, Burrum (W. H. Rands). 
 
 E, 
 
 5 ee eee 
 
 * Pal. Indica (Cre Pelecyp.), 1870, i.,'Pt. 1-4, t. 1, f. 8. 
 
CHAPTER XXV. 
 THE TRIAS-JURA SYSTEM—continued. 
 
 THE IPSWICH FORMATION (UPPER TRIAS-JURA), IN THE TYPE DISTRICT. 
 
 An area of about twelve thousand square miles in the south-eastern corner of 
 Queensland is occupied by the Ipswich Coal Field. Its strata consist for the most part 
 of fine conglomerates, grits, white, grey, and brown sandstones and shales, with a number 
 of coal-seams and beds of fireclay. 
 
 At or near the base of the formation, asseen in the neighbourhood of Brisbane, 
 is a rock consisting of a felspathic matrix, with blebs of quartz and some crystals of 
 orthoclase felspar, and containing pebbles of micaceous schist and quartz, which, towards 
 its base, attain the size of boulders. It is generaily white or yellowish-white in colour, 
 although in places it has green, purple, or brown tints. Near its base it contains pieces 
 of silicified and carbonised wood. This rock, which is easily worked, yet tough and 
 durable, has been employed ever since the founding of the City as a building store, 
 although in modern buildings it is now, to a great extent, superseded by the sandstones 
 of Murphy’s Creek, &e., which also belong to the Ipswich Formation. It is obviously a 
 clastic rock, although felspar crystals and quartz blebs have been developed in it subse- 
 quent to its deposition. ‘It has a rude sort of stratification, and its true nature can best 
 be observed on weathered surfaces. It was formerly classed as a porphyry, and regarded 
 as being intrusive through the schists, &c., which crop out in adjoining portions of the 
 City ; but there can be little doubt that it is in reality a volcanic ash. 
 
 In the road cutting in Ann Street the ash or ashy sandstone dips at 18°, and is 
 separated by thirty one inches of light and dark-coloured shales from the older micaceous 
 schists on which the shales lie unconformably. Near the Children’s Hospital, a con- 
 glomerate intervenes between the ash and the schists.* 
 
 In the immediate neighbourhood of Brisbane the Ipswich Formation has not yet 
 furnished any coal-seams of great importance. In a well at Kedron Lodge the strata 
 observed between the depths of twenty five and forty feet were alternate layers of coal 
 and fireclay, the former never over one foot in thickness. Small coal-seams have been 
 met with in shafts at Ballinger’s, about three miles north of Kedron Brook. 
 
 In a bore in search of artesian water at the Racecourse, or ‘ Eagle Farm,” in 
 1889, ‘down to a depth of six hundred and fifty feet, the strata passed through were 
 blue and grey sandstones, and shales in alternate layers. From six hundred and fifty 
 feet to six hundred and seventy feet a bed of carbonaceous shale, with layers of sand- 
 stone, and three seams of coal, was passed through. From six hundred and seventy 
 feet shale and sandstone, with layers of coarse gravel, were pierced, till at a depth of 
 seven hundred and ninety feet, a seam of good coal was met with, which, so far as could 
 be judged by the nature of the drilling and the sludge brought up in the pumps, has a 
 thickness of five or six feet. Below this seam a carbonaceous shale, sandstone, and 
 thinner seams of coal, from six inches to three feet in thickness, have been passed 
 through, down to the depth of eight hundred and seventy five feet.” 
 
 
 
 * Report to accompany Geological Map of the City of Brisbane and its Environs. By W. H. Rands. 
 Brisbane: by Authority: 1887. 
 + Report of Mr, William McKinnon, Overseer to the Hydraulic Engineer, 18th June, 1889, 
 
 Ww 
 
“A good supply of water was struck at ninety feet, in sandstone, and it rose to 
 about fifteen feet from the surface.”* A stronger supply of water was met with at a 
 depth of fifteen hundred and thirty-five feet, in sandstone, which, without doubt, was 
 artesian, and as it flowed over the casing it was noticed to be accompanied by a supply 
 of inflammable gas. When the bore was about seventeen hundred and seven feet deep, 
 the flow reached its maximum, the measurements made indicating that the discharge 
 registered two hundred gallons in thirty-five minutes at a height of three feet nine 
 inches above the natural surface.” + 
 
 From Mr. Henderson’s Report, it appears further that the junction of the base 
 of the Ipswich Formation with the underlying tale-schists was met with at the depth 
 of sixteen hundred and eighty feet. The bore was continued in the latter for a further 
 depth of ninety feet. Mr. Henry G. Stokes, of Brisbane, informed me that he 
 recognised the ashy sandstone at the base of the Ipswich Beds in the dédris from the 
 
 bore. 
 The Report of Mr. Robert Mar, F.C.S., Government Analyst, on the water of the 
 
 bore (dated 4th October, 1889), is as follows :— 
 
 Grains per Gallon. 
 
 “Total dissolved solids 113°40 
 Organic matter Trace 
 Chlorine 35°01 
 Nitric acid None 
 Sulphuric acid 0°21 
 Ammonia ... Trace 
 
 Trace 
 
 Albuminoid ammonia oe fe 
 Har fees ars 
 
 “The dissolved solids consist chiefly of chlorides and carbonates of sodium aie 
 potassium, together with a smaller quantity of carbonate of calcium and a trace of 
 
 sulphate of potassium. 
 “A small quantity of gas was in the bottle containing the sample of water. This 
 
 I tested, and found it to be ourbanetted hydrogen. 
 ‘““The water is unfit for domestic use, and indeed, in its present condition, could 
 not be advantageously used for any purpose, but by proper treatment it could be made 
 
 fit for the purpose of irrigation.” 
 On the coal from the Bore, Mr. Mar reported (Brisbane Courier, 6th July, 
 
 1889) the following analysis :—Water, 0°65 ; coke, 6415; carbon, hydrogen, oxygen, 
 nitrogen, and sulphur, 75°4; ash, 24°6; specific gravity, 1°55 
 
 Near the Albion, a fine white sandstone, similar to that of Goodna, is worked 
 for building purposes in Petrie’s Quarry. Here there is the following section :—t 
 
 Ft. in. 
 Grey sandstone ... 17e0 
 Grey shale with plants 2 4 
 White sandstone ' L730 
 Brown shales with plants 5 0 
 
 White sandstone. 
 Conglomerate. 
 Clay. 
 Among the fossil plants from this quarry my Colleague recognised Thinnfeldia 
 odontopteroides, var. falcata, Ten. Woods. 
 
 
 
 * Thid. 
 + Report to the Colonial Treasurer, by J. B. Henderson, Hydraulic Engineer, Brisbane, 18th 
 
 September, 1889. 
 { Rands’ Report to accompany Geol. Map of Brisbane, &e, 
 
 
 
323 
 
 In a bore for artesian water, south of Laidley Railway Station, samples sub- 
 mitted to me from between the depths of two thousand and four and two thousand 
 and fifteen feet were of sandstones and shales. In this bore, the contractor informed 
 me that the first fifteen hundred feet were sandstone ; from fifteen hundred to seventeen 
 hundred feet, shale with hard bands; at seventeen hundred feet, a coal-seam six feet 
 thick; from seventeen hundred to two thousand feet, shale and “quartzite,” and from two 
 thousand to two thousand three hundred and eighty feet, hard sandstone with black 
 specks. The material I saw pumped from the latter depth when I visited the bore on 
 17th April, 1890, was the débris of a fine-grained hard sandstone with carbonaceous 
 specks. The thickness of the Ipswich Coal Measures at Laidley is therefore at least 
 two thousand three hundred and eighty feet, and as I am inclined to regard the coal- 
 seam met with at seventeen hundred feet as one of the uppermost of those worked at 
 Walloon and Ipswich, the total thickness is probably very much greater. 
 
 When the coal-seam was struck in the bore a considerable quantity of gas rose 
 to the surface. Nothing was ascertained as to the nature of the gas beyond the fact 
 that it was not combustible. The water rose to twenty five feet from the surface, and 
 even overflowed while the rods were being withdrawn, owing to the expansion of the gas. 
 Mr. Henderson informed me (in a letter dated 13th January, 1890), that as the boring 
 progressed the water receded fora few days to the level of the coal-seam, and after- 
 wards rose to about seventy feet from the surface. 
 
 When I visited the bore, I was much struck by the evidently large quantity of 
 gas with which the water was charged. The sludge-pump was wound up from the 
 bottom in exactly five minutes, and therefore must have travelled at an average rate of 
 four hundred and seventy six feet per minute. A tube full of water, although open at 
 the top, must, when hauled up at this speed through a column of water, be subjected to 
 a pressure sufficient to practically seal it. When the pump was landed, the relief from 
 pressure was marked by the bubbling of the water, which splashed over the top for 
 about a minute. 
 
 On 8rd July, 1890, I received from Mr. Henderson, Hydraulic Engineer, a sample, 
 taken from the Laidley Bore at a depth of two thousand four hundred and eighty feet. 
 It was an indurated mudstone, very like some which occur in the Rolling Downs 
 Formation. Mr. Henderson informed me that about that date the water was over- 
 flowing at the rate of from fifteen hundred to two thousand gallons per diem. On 
 27th September I received from Mr. Henderson a small sample, from two thousand five 
 hundred and eight feet, of fine drillings, apparently the débris of a sandy limestone, 
 probably from the Ipswich Coal Measures, and not from the underlying Rolling Downs 
 Formation, as the previous sample had led me to believe. The bore has since been 
 abandoned, without any considerable supply of water having been struck. 
 
 The fossil plants referred to by Dr. O. Feistmantel as coming from the 
 “Talgai Diggings, Condamine River,’ are, as quoted by my Colleague :—Teniopteris 
 Daintreet, McCoy, Sagenopteris rhotfolia (Presl.), Feist., and Otozamites Mandeslohi 
 Kurr. Lest the designation of the locality should create a mistaken impression, it 
 may be well to quote from Mr. D’Oyley Aplin’s early Reports,* his descriptions of the 
 district from which the fossils were derived. 
 
 Progress Report.—“ The auriferous rocks of Talgai are confined to the Mount 
 Gammie Range and the various spurs branching from it towards Thane’s Creek, on 
 the west as far as the Sugar Loaf, and towards the Condamine on the east as far as 
 
 
 
 * Progress Report of the Government Geologist for South Queensland. Brisbane: by Authority: 
 1869. And Report onthe Auriferous Country of the Upper Condamine, &c. Brisbane: by Authority : 1869, 
 
324 
 
 the head of ‘Darkie’s Flat.’ These rocks, however, do not extend uninterruptedly 
 from the range to both waters mentioned. To the north-west of Mount Gammie, sand- 
 stones, conglomerates, and occasionally shales, belonging to the Ipswich Coal Measures, 
 stretch from near the Miner’s Creek Bridge to within less than a mile of the old 
 Talgai Township, and, continuing along the foot of the range, follow the south-west 
 branch of Mocatta Creek to within a mile of the Condamine. On the south-east side 
 of the range also, a patch of the same kind of rock, but of small extent, occurs close 
 to the west boundary of the township of Pratten.”’ 
 
 The junction of the auriferous rocks with the [Ipswich] Coal Measures is spoken 
 of by Aplin* as occurring ‘‘on the west side of the divide between Thane’s and Canal 
 Creeks.” 
 
 Report on the Auriferous Country of the Upper Condamine, §ce.—In sinking a 
 shaft about one mile from the old Talgai Township, a coal-seam was said to have been 
 struck. ‘‘ On the authority of one of the men who were engaged in putting down the 
 shaft, the thickness of the coal was from eight to ten feet. The reason assigned for 
 there being no evidence of so.thick a seam cut through and brought to the’ surface 
 was that the coal was consumed by his party while sinking the remaining one 
 hundred and fifty feet, the coal having been struck at seventy feet. Judging of 
 its quality from the few fragments lying near the shaft, there would appear to have 
 been a good deal of black shaly material associated with a clean, bright-looking coal.” 
 
 In 1887 Mr. Rands described + as follows, the Ipswich Coal Measures of the 
 neighbourhood of Beenleigh :— 
 
 “The boundary of the Coal Measures runs in a south-south-east direction from 
 Kingston Railway Station, the beds extending away in a westerly direction towards 
 Goodna and Ipswich. 
 
 “The measures consist of a series of sandstones, shales, clays, and seams of 
 coal ; the beds are lying very flat and gently undulate, the direction of the dip varying 
 in different places. 
 
 “ The following is a description of the places where the indications of coal were 
 pointed out to me, starting from north of Beenleigh :— 
 
 ‘“Shailer’s Selection (No. 261).—An outcrop of coal and black carbonaceous 
 shale occurs in the bed of a gully running into Slack’s Creek. The section is partly 
 hidden by water; it is from twelve to thirteen feet thick, and consists of alternate 
 layers of coal and a very carbonaceous shale, with one small band of sandstone about 
 four inches thick. 
 
 “The bottom portion is said to contain the best coal. From this part I broke off a 
 few large lumps of hard bright coal. The thickest coal without bands of shale is from 
 fifteen to eighteen inches thick. The bed is dipping about 6° to N. 35° E. in the 
 direction of the top of the ridge, where the boundary line of the schists occurs, about 
 half-a-mile distant. . . . I brought away a piece of this coal for analysis. It gayve— 
 
 Per cent. 
 Moisture ., - toa ite wie aa Ps a tl 
 Volatile hydrocarbons _... + 300 Ar Sas .. 24/14 
 Fixed carbon a ie ve i as ics ... 60°31) Coke 74°86 per 
 Ash... of ba ap oe ae oe ve w. 24°85 D cent. 
 100°00 
 
 The coke was brittle and compact, the ash light-grey in colour. The ash is naturally 
 very high in asample of coal taken from the outerop of a seam. 
 
 
 
 
 
 
 
 * Loe. cit. 
 + Report by W. H. Rands on the Geology, &c., of the Country in the Neighbourhood of Beenleigh, and 
 
 of the T-ogan and Albert Rivers. Brisbane ; by Authority : 1887. 
 
325 
 
 “In Dennis’ Selection (121), a thin seam of coal is visible in a gully. The section 
 here consists of— 
 
 Ft. in. 
 Black carbonaceous shale., rio A 
 Argillaceous and porianaiccte saudetone TQ 
 Deva sandy shale oy ted oo sin Fes 5 0 
 Coal.. “re er es 0 6 
 Fissile grey siee a Wi os BS, a ae fhicknete unknown 
 
 Beneath, again, is a thick bed of yellow sandstone. The dip of the strata here is 5° 
 N. 35° E. 
 
 “In Selection 393, close to the Railway, two men are sinking a shaft, which 
 is now sixty feet deep, in search of coal. The dip here is onein teu or twelve to the east. 
 They pass through— 
 
 Ft. in. 
 
 Sandstone and shale, with bands of ironstone : mi ee OO) 
 Black shale, with thin seams of coal (1 to 2 in, Pick) Kp ee Lou 
 Black carbonaceous shales containing Pecopteris ... Sis sbi 9 0 
 Hard grey sandstone (not yet through) fi oe oe re 3 0 
 
 The above thicknesses are only approximate. 
 
 “Shales and sandstones belonging to the Coal Measures dip north-east in a 
 cutting on the Railway line north of Kingston Railway Station. Mr. Charles Kingston 
 has done a little prospecting for coal on Scrubby Creek (selection 266). In a hole 
 seventeen feet deep, two six-inch seams were cut; anda little further west, in a cutting 
 in the bank (now nearly full of water), a shale full of streaks of coal can beseen. Mr. 
 Kingston informed me that in the bottom of the cutting a sixteen-inch seam of coal was 
 met with. Several outcrops of shale and coal are to be seen when the creek is dry. Dip, 
 TeoW. 1078. 
 
 “ Three and a half miles south of Scrubby Creek, in Selection 56, a seam of coal, 
 fifteen inches thick, is said to have been met with in a drive put into the steep bank of 
 the Logan River. A small seam, a few inches thick, outcrops in a gully close by. Dip, 
 7 W.N.MW. 
 
 ‘About a mile higher up, and on the opposite or eastern side of the river, a good 
 section is visible in the steep bank. The strata dip very slightly east-north-east and 
 consist of— 
 
 ARey shale 
 
 Thin-bedded sandstone and shale with thin beds of coal and ey, 
 about ... ve oe os “ef <A nd 15 0 
 Black band and aialee oh, 6 O 
 Black band with bed of i impure eal 12 riches thick os 5 6 
 White clay ap: wee am oy 0 8 
 
 Black band ad alilad: 
 
 Three-quarters of a mile south-west from the river here, a shaft was sunk, forty feet 
 in depth, on Selection 261, by a man named Smith. Carbonaceous shales with streaks 
 of coal were passed through. At forty feet, a seam of coal was struck. Mr. Smith 
 and another man working with him were suffocated on descending the shaft by foul air 
 which had collected at the bottom. Since this fatality, which happened some months 
 ago, no further sinking has been done to test the thickness of the seam. The shaft is 
 close to the boundary of the Coal Measures. 
 
 “Mr. Downman has done more than anyone in the district towards proving 
 the presence of payable seams of coal by putting down a borehole to the depth of two 
 hundred and ninety one feet near the centre of his Selection (No. 68). Mr. Falconer 
 
326 
 superintended the putting down of the borehole; the borer used was a steel cutter. The 
 
 size of the cores brought up was about three inches in diameter near the surface, and 
 two inches lower down :— 
 
 Thickness. Depth. 
 Ft. in. Ft. in. 
 
 Surface ... bse A ave _ Ae Be HR oe: noe 72 8 
 Shale : eon LO ; 74 2 
 Shale 44 2 6 76 8 
 White sandstone 4 6 81 2 
 Sandstone and shale By (9 86 8 
 Sandstone hs we Bee ave 2 0 88 8 
 Black shale 4 0 92 8 
 Light shale dae6 94 2 
 Shale .... 2 3 96 5 
 Black shale 5 9 102 2 
 Shale a ate: 2 0 104 2 
 Sandstone and quart a 8 19) 105 2 
 Grey sandstone.. 12 0 We oe 
 Coal ee 4 0 160 8 
 Black shale ma can 12S 129 4 
 Black shale ; O 10 130 2 
 Calcareous sandstone ... 2 6 isi) 
 Black shale 5 O 137s 
 Shale and sandstone 1970 156 8 
 Coal 4 O 160 8 
 Shale LS 162 4 
 Hard siliceous ara 10 163 4 
 Shale 6 0 169 4 
 Coal bp Ons 169 7 
 Black sandstone Tea 180 7 
 Shale 6 4 186 11 
 Coal 4 1 191 O 
 Sandstone 9 O 200 O 
 Blue fossiliferous aioe 1 a) 211 0 
 Fireclay .. 0 2 211 2 
 Shale 7 A 218 6 
 Fireclay ... 0 11 219 5 
 Grey sandstone 21 3 240 8 
 Fireclay .. 0 3 240 11 
 Hard grey ‘sandstone and shale 19 5 260 4. 
 Coal Ae ; 2; O 4 260 8 
 Shale oe. 48 262 10 
 Coal with bance of ete “i LG 264 4 
 Good hard coal... 5 3 269 7 
 Shale Ores 269 10 
 Fireclay .. 0 2 270 O 
 Shale St ads. of Roar 5 6 275 6 
 Fireclay ... 1 4 276 10 
 Coal se a AD 278 10 
 Black band 0 8 279 6 
 Coal ake 53 284 9 
 Hard sandstone ‘ae 284 11 
 Coal ee Ome 285 3 
 Hard sandstone 0 8 285 11 
 Hard sandstone with banda of uvonatone Samed! 291 O 
 
327 
 
 “ According to this return, therefore, there were four seams of coal of sufficient 
 thickness to pay to work passed through in the boring—viz., a four feet seam at one 
 hundred and sixty feet in depth, a four feet one inch seam at one hundred and ninety 
 one feet, a five feet three inch seam at two hundred and sixty nine feet, and a seven 
 feet eleven inch seam (including eight inches of band) at two hundred and seventy eight 
 feet in depth. Unfortunately none of the cores of coal were kept, so that I was unable 
 to see the quality of the coal. 
 
 ‘““A sample of the bottom seam (the seven feet eleven inch seam) was sent to 
 Mr. A. C. Gregory, who reports as follows :— 
 
 Per cent. 
 ‘ Fixed carbon... ne sth sac Ae Ber ae sey soo Bis 
 Volatile in coking... ari nate ome Be AB 568 55 PaaS 
 Agh? 7s); Ae Pi Ree 9:0) 
 
 A fair coal for steam purposes aad bemechold use, ale for smith’s work. The high 
 percentage of ash is probably due to débris from the boring being mixed with it.’ This 
 coal would answer admirably where an avoidance of smoke was an object, as the 
 percentage of the volatile hydrocarbons is small. The site of the borehole is only 
 about ten or fifteen chains from the Logan River. Mr. Downman tells me that 
 steamers of two hundred tons burden have come up the river to this point for the 
 purpose of carrying away timber, so that there would be no difficulty in the way of the 
 conveyance of the coal to the Brisbane market. 
 
 “At present the nearest available Railway Station is Kingston, about seven miles 
 distant. The Logan Village line passes about half-a-mile from the spot, but it is on the 
 opposite side of the Logan River. 
 
 *T was informed by Mr. Downman that coal can be seen outcropping in 
 Chambers Creek, in the same Selection, when the water is low. 
 
 “Mr. Watt accompanied me to his Selection (No. 11), three miles south-east of 
 the Logan Village, where the following section of rocks is exposed in a gully :— 
 
 Ft. in. 
 Fine-grained brown sandstone _... wi oe ae rae or 
 Black shale, with bands of coal and Ben as ak Pree oie! 
 Black and brown shales, with coal and an bands of sathiaeons ae tw 
 
 The dip is 8° W.S.W. A shaft forty seven feet in depth has been sunk in the 
 gully close to the base of the black and brown shales. A seam of cannel coal, about a 
 foot thick, was cut near the top of the shaft, and, lower down, a seam of coal about 
 fifteen inches in thickness. A proximate analysis of a piece of this coal is appended :— 
 
 
 
 Per cex . 
 Moisture... ey as ite Sor she wae sea key 
 Volatile Bydesoarhori Be a i se 500 SGC scq US RCAL 
 Fixed carbon wae ae ar Ae ea ane es . «40°37 
 INES ces ae ae Bak ae ee re ele AS sos alleen 
 
 100:00 
 
 The coke was hard and somewhat compact; the ash was of a slightly reddish-grey 
 colour. The coal was hard and bright, with thin scales of silica on its faces; this 
 would account for the high percentage of ash. These scales of silica would probably 
 not occur at any depth from the surface. In testing this ground for coal, it would be 
 better to sink or bore lower down the gully, on the flat to the dip of the beds. 
 
 “On the top of the ridge at the head of this gully there is a bed of freestone at 
 least one hundred and three feet thick. Mr. Watt has had some specimens of this 
 stone faced ; it would make an excellent building stone, being hard and durable. This 
 ridge extends right across the Albert River. 
 
328 
 
 “Following up Sandy Creek, from its junction with the Albert River to Mount 
 
 Tambourine, brown and yellow sandstone, with here and there shales with streaks of 
 coal, occur. Mount Tambourine itself consists of leucitic basalt, overlying the Coal 
 Measures sandstone. At the head of this creek a fine section of this basalt is seen, 
 where the water, falling from a height of about one hundred feet, has made a cutting 
 through it. I was informed that the outerop of a thick seam of coal is visible in 
 Flagstone Creek, twenty miles south of Beenleigh.” 
 
 In his “ Report on the Albert and Logan district,” * Mr. Rands added the follow- 
 ing notes :-— 
 
 ‘The boundary between the Ipswich beds and the schists runs in a north-north- 
 westerly direction from the heads of Nerang Creek to Mount Tambourine; it passes 
 under the basalt of that mountain, and then continues in the same direction, running 
 between Sandy and Cedar Creeks, and crossing the Albert River about a mile above its 
 junction with Cedar Creek. It continues on in the same direction for about six miles, 
 and then bends to the north, crossing the Railway Line and the Logan River near the 
 village of Waterford. From thence it runs in a north-westerly direction to Kingston 
 Railway Station, and then in a north-easterly direction to Mount Cotton, from which 
 place it runs in a south-easterly direction to Alberton and Ageston. 
 
 “The beds consist of a series of sandstones, shales, and clays, with seams of coal. 
 
 The beds dip generally at a low angle; the direction ame amount of the dip in various 
 places is shown on the map. 
 
 “At Ageston the country is covered with alluvial deposits; coal was met with 
 below the ellaviomn, ina borehole on Mr. W. H. Couldery’s property, in Selection No. 2. 
 
 ‘““In my Report on the Beenleigh District, 1887, I described these beds and the 
 outcrops of coal that occur from Tambourine Mountain, as far north as Shailer’s 
 Selection, No. 261. 
 
 “‘ Hearing that Mr. Watt had opened up another seam of coal, I revisited his 
 Selection No. 11. A drive sixteen feet long has been put in on a seam of coal which 
 lies immediately beneath the freestone mentioned in my last Report. The section seen 
 here is :— 
 
 Ft. in. 
 Freestone ... z bie ive Te 50 O 
 Black horace guns eis Eirenke of Pa 0 4 
 Light yellowish clay ; 0 6 
 Dark brown laminated shale w ith coal aid sahdetond 1AM 
 Coal with a thin streak of clay ... 0 53 
 Clay-band ... : OBL 
 Goals... O 43 
 Clay-band ... ie ; OFal 
 Coal... A pe A Om2s 
 Clay-band ... oe He ee 03 
 Coal... ese i Ree L 0 
 Dark hard band ... ... 0 2 
 Coal soe fin ic 0 8 
 Thin laminated PanOctore OG 
 
 Shale (coaly). 
 
 The seam is, therefore, three feet three and a half inches thick, including seven 
 inches of bands. Unless these bands which are distributed ee hoat the seam thin 
 out, the coal will be of no commercial value. The dip of the strata here is south-west 
 
 
 
 * Brisbane: by Authority : 1889, 
 
329 
 
 at 8°. The coal is situated at the head of a gully about a hundred yards north- 
 west of the shaft mentioned in my previous Report. The following is a proximate 
 analysis of this coal :—- 
 
 é Per cent. 
 Moisture... Sie AK sie ane es -” a ee 22 
 Volatile hydrocarbons _,.. bf Sor 380 wae Stic wm 220 
 Fixed carbon a os 50 ae a ah ane sq UR, 
 Ash aN ae be es Th ee ne a eo 9 ee 
 1000 
 
 The coal cakes well on coking. The ash is light-grey in colour. The coke was much 
 swollen up, soft, and black-co!loured. The coal is laminated and friable. 
 “The analysis of the coal from the shaft was :— 
 
 
 
 Per cent. 
 Moisture... ine site ri mt 1% xe si me ioe 
 Volatile hydrocarbons... oe wee vies os uke ie 70 
 Fixed carbon mi ref ee = a be an wee 49°37 
 Ashes ahs ts Se ser Ads fe AAD sc SOLS Ol 
 100°00 
 
 The coke was hard and compact, and the ash of a slightly reddish-grey colour. 
 The high percentage of ash is probably due to the samples, in both cases, being taken 
 from close to the surface. 
 
 “The freestone overlying the coal is of a good white colour, medium in grain. 
 It lies in beds averaging about four feet in thickness. Some of the layers are too 
 laminated to make a good building stone, but others are massive and hard, and 
 would make a good facing stone, though it is perhaps too coarse for fine mouldings. 
 Stone from this ridge, which runs across to the Logan, was used for building a 
 chimney in the Logan Village about twenty-three years ago. The stone has withstood 
 the weathering action of the atmosphere well. 
 
 “A borehole was put down on the Timber Reserve, about two miles north of the 
 Logan Village, to a depth of three hundred and fifty feet. After passing through the 
 Ipswich beds, the schists were struck in the bottom of the bore. No thick coal was 
 met with. 
 
 “In the cuttings on the Railway, between the Logan Village and Jimboomba, 
 nothing but sandstones and shales are visible. Close to Jimboomba, the sandstone is 
 thick-bedded and nodular. 
 
 “In Goertz’s Selection (No. 20) about three miles south of Jimboomba, I was 
 shown a bed of highly carbonaceous shale, containing streaks of coal, which had been 
 mistaken for a seam of coal. 
 
 “The country in the neighbourhood of Tambourine consists almost entirely of 
 brown sandstones. 
 
 “From Tambourine up to Lahey’s Mill, on Cunungra Creek, nothing but 
 sandstone ridges and black-soil flats are traversed. The higher ridges on either side of 
 the creek are capped with basalt; while, six miles above the mill, the country is 
 almost entirely of basalt. 
 
 ““Mr. Paine accompanied me over a low gap in the Darlington Range, where 
 there is a break in the basalt, on to the heads of the Coomera River. The country was 
 all sandstone. 
 
 “On Back Pine Creek, there is a section of blue and black carbonaceous 
 
 shale, with streaks of coal, overlying a hardened sandstone, and dipping south-west 
 at 15°, 
 
330 
 
 “Close to Pine Creek, near Selection 31, there is a hill called Meerschaum 
 Mountain, from the fact that a very light white material, somewhat resembling that 
 mineral, can be picked up on its sides. I have not seen this substance in situ. This 
 substance is an infusorial earth. Mr. W. A. Dixon, of Sydney, gives the following 
 analysis of it :— 
 
 
 
 Per cent. 
 Moisture and traces of organic matter ... x0 aes re Pr E Osa 
 Oxide of iron and traces of alumina ... a8 586 re ie 0°59 
 Lime ee Te abe dee wee nae vee Aap ve. traces. 
 Silica si fen oes wae Ser wee at as eo OnOm 
 
 100-00 
 
 Mr. Dixon says that under the microscope the silica is almost entirely composed of 
 the frustales of diatoms—probably MMelostra arenaria. I confirmed Mr. Dixon’s 
 remarks as far as the microscopical examination went. 
 
 “Returning to Tambourine, I next visited Mr. G. A. Ball’s Selection (No. 71), on 
 Flagstone Creek, where a seam of coal, about two feet six inches thick, crops out-in the 
 banks of the creek. A section across the seam shows :— 
 
 Fb; in: 
 Colleen. ay - sak ext ax He ate HA oe koe 
 Coaly shale... me ne ee whe bi on is Pe AOR 
 Coal... iA ess ia st “ aa es Mtr ipa te 
 Clay band see ae va oe a aes dos UE 
 Coal te Sc ri * ps ie ear: roe pORLO 
 Coarse grey sandstone ih +7 oe, ae oe a pork vi 
 
 “A small fault, running N. 15° ‘W., across the creek, displaces the seam 
 about two feet. The coal dips 8S. 30° W. at 12°. 
 
 “The following is a proximate analysis of a sample of the coal taken from the 
 cleanest part of the seam :— 
 
 Per cent. 
 Moisture AB Ae ner aes is ee ae ee me ehh 
 Volatile hydrocarbons pes Eye a ie ze oe iy otto 
 Fixed carbons Pe oa “ee Bee Rac ay ire POUL A 
 FAS han mess a ats fas ass ee ao a ae sh ORS 
 
 100°0 
 
 The coal is a bright non-caking coal; the ash is white. 
 
 “The small range between Flagstone Creek and Beaudesert, known as Birnam 
 Range, is of a hard silicified sandstone. On the western fall of this range a great 
 thickness of black and blue shales is visible in the gullies in Mr. W. T. Walker’s 
 selection (No. 94). 
 
 “In Mr. Rafter’s Selection (No. 63) there is a ridge of sandstone running in a 
 northerly direction. The lower part of this sandstone contains a large percentage of 
 iron. In the upper part some of the beds are very soft. I noticed one bed, about nine 
 feet thick, which was a good hard stone, and had apparently withstood weathering 
 action well. Ido not think that any of it is of sufficiently good character to pay for 
 carriage as a building stone. 
 
 ““T was afterwards informed that Mr. Jennings had opened up a small quarry in 
 his Selection to the north of Rafter’s, on the same ridge of sandstone, but unless it is 
 of a very superior quality it would not compete with the building stones at present 
 available for Brisbane. The sandstone dips to the east at 24°. 
 
331 
 
 ‘‘ Below the sandstone, and a little higher up the gully, a seam of coal, with the 
 same dip, and one foot seven inches.in thickness, crops outin the bank. It is a good, 
 bright, non-caking coal, without any bands, but it has too high an angle of dip and is 
 not thick enough to pay to work. The section in the gully shows :— 
 
 Ft. in. 
 Sandstone 0 0 
 White clay 3 m0 
 Codlaane. Ay aa yal By 
 Fireclay x 0 13 
 Laminated eaddateren Fe iD 
 “* Approximate eet of this coal gives :— 
 Per cent, 
 Moisture eee nn are oe ee: mee Ore ae. 43 
 Volatile ede eetena. Nie ee es Tes ner ae eee Lo:5 
 Fixed carbon ae nate sae me at ‘= a eae Lek: 
 Ash... Ae ap ee a aoe HM “fie iG app, GIL 
 100°0 
 
 The ash was of a dark-grey colour. 
 
 “A seam of coal crops out in a gully, in Selection No. 137, belonging to Mr. 
 Brayford, about a mile and a half north of Beaudesert. The section in the 
 gully is :— 
 
 >) 
 
 SVs) (Sia Siene eS tSe 
 
 = 
 = 
 i= 
 
 ia oe St 
 
 Fireclay : 
 
 Black shale wih Srenee of coal 
 
 Fireclay ; 
 
 Black shale aitle aiesics of pia 
 
 Fireclay ee ire ae ames 5 as 
 
 Coal... re as ae os nce 
 
 Fireclay 
 
 Brown shale 
 
 Bright clean coal yer nee ne a Age ee ap 
 Fireclay ord er aoe a A ee ~~ ans er 
 Coal... th ree see aie ee a See sae tae 
 
 H 
 
 m Cr co Go Oe 
 
 role 
 
 ie} 
 
 63 
 
 This is one of the best-looking coals I saw in the district. The dip of the coal is 
 W. 10° N. at 10°. I appended analyses of two samples of this coal, one taken from 
 the outcrop in the gully, and analysed by Mr. Joseph Fletcher, the other from a shaft 
 in Mr. John Waters’ Selection (No. 120), and analysed by myself :— 
 
 Sample from Sample from 
 Sample. outcrop. shaft. 
 Per cent. Per cent. 
 Moisture Ae ee eke nae Not determined 
 Hydrocarbons Goiniio ea we 840 a 440 (includes moisture) 
 Fixed carbons ... ae 562 ae BENG) nee 47°3 
 Ash eee sid nee si eb ae 87 
 100°0 100°0 
 
 The ash was white. The coal is hard, and has a specific gravity of 1:41. It resembles 
 a cannel coal and burns freely. 
 
 “ The shaft in Mr. John Waters’ Selection was filled in, but I was informed that 
 the coal was much thicker there. 
 
 “ Another seam crops out about a hundred yards higher up the gully, ‘This is 
 very impure coal; it is more of a coaly shale. 
 
332 
 
 “From Beaudesert I went up the Logan and Palm Creek to within three or 
 four miles of Mount Stanley, about thirty miles south of Beaudesert. The Ipswich beds 
 extended all the way up. I saw no seams of coal. In Mr. Byrne’s Selection, on Palm 
 Creek, I was shown a bed of black carbonaceous shale, about fifteen inches in thickness, 
 which had been mistaken for coal. 
 
 ‘Seams of coal have been reported to exist in Christmas and Widgee Creeks, 
 but as I could get no definite information regarding them, TU did not visit that part of 
 the country. 
 
 “ Nothing, it will be observed, has been attempted in the way of trying any of 
 these seams away from their outcrops; the seams are, in no case, of any great thickness, 
 but the analyses of some of the coals show them to be of a fair quality, and 1 think it 
 would repay the owners of the properties to test them at a shallow depth away from the 
 outcrops. 
 
 “T believe that Mr. Downman has done nothing at present to verify, by means 
 of a shaft, the correctness of the results obtained in a borehole put down by Mr. 
 Falconer, a section of which I gave in my previous Report.”’ 
 
 J. 
 
CHAPTER XXVI. 
 
 THE TRIAS-JURA SYSTEM—continued. 
 THE IPSWICH FORMATION (UPPER TRIAS-JURA) IN THE TYPE DISTRIOT—continued. 
 
 In and near the Town of Ipswich, the strata are tilted at high angles, and are 
 accompanied by flows of basalt. I cannot, however, see any clear evidence that the 
 tilting of the strata is due to the igneous rocks. On the contrary, there is every 
 appearance of the latter being interbedded with the former, and having been tilted 
 simultaneously with them.* On the summit of Limestone Hill, within the Town 
 boundary, two beds of limestone are seen, the uppermost being about ten feet thick, 
 and resting on thirty feet of grey and reddish shales. Beneath the shales is a thick 
 bed of basalt, which, again, rests on a thick bed of limestone. A second mass of basalt 
 is seen beneath the lower limestone bed. The limestones dip at a high angle to the 
 north-east. Iam inclined to believe that the upper bed of limestone is, so to speak, 
 “conformably” overlaid by a thick basalt, which, at first dipping with the same high 
 angle as the limestones and shales, gradually flattens out eastward, till its base again 
 rises to the surface on the left bank of Bundamba Creek. The limestone, as seen at its 
 outcrop, is rather the siliceous skeleton of a sandy limestone, and contains frequent 
 kernels of chert. It appears to be quite unfossiliferous. It is described by Gregory 
 as “tufaceous limestone, containing siliceous concretions.” 
 
 The most important description of the Ipswich Coal Field published up to the 
 present date, although it is one of the earliest, is that of Mr. A. C. Gregory.+ This 
 valuable Report, which I find it impossible to abridge very much, deals principally 
 with the character of the various coal-seams. The following extracts are taken from 
 the Report :— 
 
 “ Old Moggill Coal Mine.—The Moggill coal-seam being confined to a small area 
 by the river on the east and south, and by a fault on the west, the available coal was 
 soon worked out, and the mine has been abandoned for about ten years. It is stated 
 that the seam was about six feet thick, but not of a very high class, probably owing to 
 its being worked so near the outcrop. 
 
 * Mr. Lyons’ Coal Seam.—About one mile to the W.S.W. of the Old Moggill 
 Mine, several outcrops of coal are visible, and a shaft has been sunk seventy feet by 
 Mr. Lyons, on Portion 117, and a seam of coal five and a-half feet thick cut at forty-five 
 feet. The coal has several thin bands of bituminous shale, but, rejecting the bands, 
 there would be from three to four feet of good available coal. 
 
 “ Section taken from the shaft and adjacent outcrops :~— 
 
 Feet. 
 Coarse grit, irregularly stained with iron... 35 ss Sw yee) 
 Coarse conglomerate _... a ae a fer Bek ee 8 to 10 
 Coarse sandstone = ne at ae AS oe non eee) 
 Hard shales se ee a Se eas ee ee Bes ee lb 
 Coal seh ae me A su ve ey te ane w. OF 
 Thin-bedded sandstones and shales... we nit ane oo eck OU 
 Coal ‘ait aie ey te se oes or si “ite ‘oem we 
 Thick-bedded coarse sandstones es ahh te ae ... over 50 
 
 
 
 * See Plate 49, fig. 1. 
 + Report on the Coal Deposits of the West Moreton and Darling Downs District. Brisbane: by 
 Authority ; 1876. - 
 
334 
 
 “ The strata are nearly horizontal, having a very slight dip to the south-west. 
 
 “Following down the gully three-quarters of a mile, there are several small seams 
 in the bottom of the watercourse, and on the southern bank a seam of coal eight feet 
 thick is exposed. 
 
 “On the bank of the river, three-quarters of a mile east of the shaft, there is a 
 seam of coal, one and a-half feet thick, at the water level. 
 
 “Taking into consideration the relative positions of the outcrop of these seams, it 
 may be inferred that the coal in Mr. Lyons’ shaft is the uppermost bed, and that there 
 is a small seam some fifty feet lower, and a thick workable seam a hundred feet deeper, 
 a portion of which, being thrown up by a fault, was worked at the old Moggill Mine. 
 
 “The coal is bituminous, moderately hard, cakes a little in coking. Specific 
 gravity, 1°52. A specimen of the better part of the seam gave :— 
 
 Volatile in coking... sie ay: a at te oe Seo tits) 
 Fixed carbon ... ae ae sae ae eh nee ar. see rol 
 Ash ioe ae as Riis aoe axe ae rae as ae wel at 
 
 SWE cae ae re ee 100 
 
 “ Goodna Mine.—Crossing the Brisbane River, some thin bands of inferior coal 
 are visible under the sandstone of Mr. Jeay’s quarry, just below Woogaroo; and at 
 Goodna a seam of coal crops out, less than a mile from the river. 
 
 “This seam, which dips from 3° to 5° to the southward, was originally 
 worked from the outcrop, but now by a shaft ninety feet deep, through sand- 
 stone and inferior bands of coal, the workable portion being about four and a-half feet 
 thick. This mine has been extensively worked for about eight years, and has furnished 
 a large proportion of the coal supplied to the steamers on the river and intercolonial 
 traffic. 
 
 “The coal is of fair quality, with bright laminar fracture, but rather tender and 
 friable. It cokes well. Specific quality, 1°47. 
 
 Volatile in coking 29 
 Fixed carbon ... oa ne ar wae oad ans he neg, kes 
 Ash we = mt ae a ee 70 ne saa types 
 
 100 
 
 “This seam of coal is apparently limited on the east by Woogaroo Creek, and on 
 the west by a fault and Redbank Creek, beyond which it again appears in the old 
 Redbank Coal Mine, extending up the River about a mile and a-half to the Six-mile 
 Creek, in which direction it deteriorates both in quality and thickness. 
 
 “ Redbank Coal Mine.—The Redbank coal-seam, though now abandoned, for 
 several years was the chief source of supply in the district. It is nearly horizontal, 
 the dip a little to the south, the thickness varying -from three to six feet, with several 
 bands of shale. The outcrop extends for half a mile along the bank of the river. The 
 coal is rather soft, and very similar to the Goodna seam, but not so free from shale and 
 band.* 
 
 “ Stv-Mile Creek.—At the Six-mile Creek, on the Ipswich Road, there is a disturb- 
 ance in the coal strata, the seams cropping out at a high angle of 80° to 40°, and the 
 coal much mixed with shale, so as to be of no value. The high angle of dip on both 
 sides of the valley is, however, only local, and the shales and sandstones to the west 
 indicate that the coal continues in that direction, with very little dip, as far as Bundamba 
 Creek, while in a southerly direction an anticlinal axis of elevation brings the coal to 
 the surface, with a dip to the north on one side and to the south on the other. 
 
 ——-—__ 
 
 
 
 
 
 * From the preceding paragraph it appears to be identical with the Goodna Seam, (R.L.J.) 
 
 € 
 
335 
 
 “ Thomas’s Mine.—At this point Thomas’s Mine has been opened on Portion 270, 
 Parish of Goodna, the workings being on a dip of 15° to the south for one hundred and 
 fifty yards. The thickness of the seam is about six feet, of which four to five feet are 
 available, as there are some bands of clay and shale, which vary considerably in 
 thickness. The coalfrom this seam is hard and bright, and bears carriage better than 
 the average of the district, while it is ia good repute as a steam coal. The specitic 
 gravity is 1°44. . 
 
 Volatile in coking... sy <p ty re nu 20) 
 
 Fixed carbon ... pa ms wae ee an ee 5 sok ma 
 
 Ash at =. ror or See A as ats oe Ae ee 
 100 
 
 “It makes a fair coke, but not equal to the coals further to the west, near 
 Ipswich. About two hundred yards to the east of Thomas’s Mine the coal crops out in 
 a gully. 
 
 “ Ooal Seam in Portion 252, Goodna.—To the south the seam dips for about a 
 mile, and then rises again at an angle of 30°, the outcrop crossing the road on the 
 north boundary of Portion 252; but a hundred yards further south it shows again in 
 a horizontal position, with a thickness of six feet, the outcrop showing along the face of 
 the hill for a quarter of a mile.* 
 
 “ Thomas's New Coal Mine.—To the south and west of this outcrop the lower beds 
 of clays and shales are uncovered for a space of about a mile, when the coarse sand- 
 stones again appear in horizontal beds, covering a fine seam of coal [the Aberdare], 
 which crops out in Portion 270, parish of Bundamba [Goodna?], where it is worked by 
 Mr. Thomas. The seam is eight to ten feet thick, but only four to five feet of workable 
 coal. At the outcrop it dips 1° to the south, but rapidly increases, and at the back of 
 the hill, two hundred yards south, the sandstones dip 10°’to the south. The coal 
 from this seam is not quite so hard as at Thomas’s Mine, Portion 270, Goodna, but 
 seems to be less mixed with inferior bands. The specific gravity is 1°40. 
 
 Volatile in coking = al Aer es aad bi: ni soo BW) 
 Fixed carbon ... aa a0 ove So TC ae Lia Oo 
 Ash she tee mia sae aes ae Sic ee ee ao Aa 
 
 100 
 
 “ Thompson's New Coal Mine.—About half a mile to the northward of Thomas’s 
 Mine, what appears to be the same seam is visible in a gully in the water reserve, and 
 a shaft has been sunk on the adjacent Portion No. 174, Bundamba [Goodna >] by J. M. 
 Thompson, Esq., and an excellent seam of coal cut at forty five feet, the dip being 17° 
 to the west. The thickness is from six to ten feet, but there are some bands of shale 
 and inferior coal which will probably reduce the workable portion to five feet. The coal 
 is of a good, bright, reedy character, but rather tender and friable. It cokes very well. 
 Specific gravity, 1°38. 
 
 Volatile in coking ... ae eh ie ty ae ae aE 32 
 Fixed carbon aa te me ves ar Ne: oe we 62 
 INGAR ape a ae ae ae sa ee cae nae ay 6 
 
 100 
 
 “This small proportion of ash and large percentage of carbon places it at the 
 head of the Ipswich coals, both as a steam coal and for coke. 
 
 
 
 
 
 
 
 * This and the seam referred to in the preceding paragraph appear to be one and the same. (R.LZ.J.) 
 
336 
 
 “The dip of the seam being to the north-west, it passes under Bundamba Creek, at 
 a distance of four hundred yards, and the opposite bank rises into an undulating tract 
 of basalt, having a length of four miles from the Bremer River south-westerly, and a 
 breadth of two miles from Bundamba Creek to the boundary of the Town of Ipswich ; 
 and as the Carboniferous strata are found to dip and pass under the basalt along the 
 whole of the margin of the igneous rock, it may be inferred that the coal beds are 
 
 only interrupted by the fissures through which the basalt has been erupted, 
 
 “Ooal at Mihi Creck.—Crossing to the north-west of the igneous tract, the 
 Carboniferous rocks are found rising to the surface in the Town of Ipswich, and several 
 small seams of inferior coal are exposed in the cuttings for railway and roads; and at 
 the junction of Mihi Creek withthe Bremer River, two large seams of coal crop out, the 
 upper being exposed in the bed of the river, the adjacent Railway Cutting, and at the top 
 of thehill on the Pine Mountain Road, the outcrop trending north-east towards the Tivoli 
 Mine. In the Railway cutting the dip is 14°to the 8.S.E. The quality of this coal is 
 inferior, and evidently much disturbed at the outcrop, and the beds of sandstone and 
 shale vary considerably in thickness in the space of a few yards. 
 
 “ Eastwood Mine.—The second seam is about a hundred feet below that exposed in 
 the Railway cutting, the outcrop showing in the gully under the Railway Bridge. It has 
 a thickness of seven feet, but there are several thin bands of shale. This seamis worked 
 at a point about three hundred yards to the N.N.E. by Messrs. Archibald, as the East- 
 wood Mine, where the dip is 7° to the S.E. The coal is bright and bituminous, but very 
 soft, and breaks small incarriage. It cokes well. Specitic gravity, 1°4. 
 
 Volatile incoking ... Src Sic sett are tex she Sete 
 Fixed carbon ... Soc ape aire vas ane fin Sac OS. 
 PNA ee 3B “96 oe 500 Sc ave Kc one ae ad by 
 
 100 
 
 “ Tivoli Mine.—Qn the line of outcrop of the upper seam, at the distance of one 
 and a-half miles, is the Tivoli Mine, which is worked by a drive of six hundred yards 
 ona dip of 14° to the S.S.E., the thickness of the seam being five to six feet. The coal is 
 bright and bituminous, very tender, breaking into small cubical pieces so easily as to 
 scarcely bear carriage. It, however, makes excellent coke. Specific gravity, 1°35. 
 
 Volatile in coking... a re Ne tes Be 4 Bog © ff 
 Fixed carbon ... ee a a “ee wae be 56 eG 
 100 
 
 ‘ Blond and Wright's Seam.—The outcrop of a thin bed of sandstone, which covers 
 the Tivoli seam, leads about a quarter of a mile east to Blond and Wright’s Mine, which 
 is worked on the same seam, on a dip of 15° to the S.S.E. The coal is a little 
 harder than at the Tivoli Mine, but in other respects not of equal value. Specific 
 gravity, 1°32. 
 
 Volatile in coking... ei sas uae sv ae si aie, P18 
 Fixed carbon .., SAF Pe =e eee stots ee a aay LU 
 Ash aw 5 me cee 45 4 a af a ote i 
 
 100 
 
 “On the north-east side of these workings a fault occurs, and the seamis thrown 
 downwards, and worked at a lower level on both sides of the road, on the descent to 
 Sandy Creek. The quality of the coal does not improve in this direction. 
 
 “New Mine.—About a quarter of a mile to the north of the Tivoli Mine, a seam 
 of coal has recently been opened, showing a thickness of eight feet, but some bands of 
 
337 
 
 inferior quality reduce the workable coal to six feet. The dip is 11° to the S.S.E., 
 and would apparently pass one hundred feet below the Tivoli seam. This seam is 
 probably identical with the seam of the Eastwood Mine. The coal is moderately hard. 
 Specific gravity, 1°34. 
 
 Volatile in coking... ts wk oe se ahs is sea Oe 
 Fixed carbon .., ba bad a oe an aa: ee ee! 
 Ash we cr Sas aes ae oe otc Ec = rpg hey 
 
 100 
 
 “Coal Seam on Brisbane River—Two miles north-west from the Tivoli Mine, 
 a large coal-seam is exposed on the bank of the Brisbane River, just above the Rocky 
 Crossing. The total thickness of the seam is nearly thirty feet, but so full of bands of 
 shale that only three feet of the lower part could be worked, and even that of such 
 inferior quality that it would be of little value as fuel. A specimen from the best part 
 of the seam gave the following results. Specific gravity, 1:47. 
 
 Volatile in coking... ae SH ak nck oc we gee 
 Fixed carbon ... Sas a ane ee a3 ee she Rag a! 
 Ash rs ae Se Ne a ae SE an re. se eat 
 
 100 
 
 “Tn the gullies to the south-east of this outcrop the coal-seam shows with a 
 reduced thickness of ten feet, of which five to six feet would be workable, though not 
 of very good quality; but it is probable that it improves to the southward, as it recedes 
 from the Pine Mountain, where the coal strata are tilted up at high angles by the older 
 serpentine rock, which forms the anticlinal axis of the mountain. 
 
 “The whole of the hereinbefore described seams of coal are of the bituminous class, 
 and are associated with coarse sandstones and arenaceous shales. The weight of evidence 
 is in favour of the assumption that the whole of the workings are confined to two main 
 seams, principally the upper one, and that the difference in the quality of the coal raised 
 from each mine has some relation to the distance from the northern margin of the 
 coalfield ; and it may be inferred that the drift from the high ranges of Devonian rocks 
 deposited more earthy matter along the margin than in the more distant and central 
 portions of the great valley in which the coal was originally formed. 
 
 “Coal near Walloon.—FYollowing the general course of the Railway from Ipswich to 
 Toowoomba, the first indications of coal are observable a little beyond Walloon Station, 
 where small blocks of coal are observable in the bed of a watercourse descending from 
 the range in the Rosewood Scrub. Coal shales are visible in banks of the gullies, and 
 just below the basaltic cap of the range beds of black carbonaceous shale are exposed, 
 while the soil is mixed with fragments of hard, bright coal, indicating the proximity of 
 a seam of good coal, though the outcrop was not found. The character of this coal is 
 quite distinct from the bituminous coals worked near Ipswich, being very hard, not 
 subject to injury by exposure to the weather, less brilliant in fracture, and does not 
 cake much in coking. The volatile portion usually exceeds forty five per cent., pro- 
 ducing a large proportion of oil or gas, according as it is subjected to a low or high 
 temperature in distillation, and it may be observed that these characters apply 
 to almost all the coal-seams to the west of this locality. The coal has a specific 
 gravity of 1°30. 
 
 Volatile in coking... he ai iG nde te a0 reat 
 Fixed carbon ae ol aoe we nee “ne aes serials 
 Ash ane ae oe at ee on ie ae wet carnage 
 
 100 
 
338 
 
 “ Coal near Rosewood Station.—Coal is reported to have been found near the Rose- 
 wood Station, but that the seam is only one and a-half feet thick, though of excellent 
 quality. About three miles beyond Rosewood, and a mile north of the Railway, two 
 small seas of coal were found in the shales on the bank of a watercourse descending 
 from the range, but neither of any value. The coal strata here rest on limestone con- 
 taining coals of the mountain limestone series,* but the actual junctions of the two 
 series of rocks were not visibie, the Carboniferous rocks being overlaid by basalt, which 
 forms the summit of the range 
 
 “ Coal on Blackfellow’s Creek. — Although the Railway cuttings through the Little 
 Liverpool Range show some good sections of ake coal sandstones He shales, no coal has 
 been found, and it seems that the coal is covered in this locality by a great thickness of 
 shales and coarse sandstones, similar to those to the east of Ipswich, and as these strata 
 dip from the summit of the range to the west, it is not till Blackfellow’s [Tenthill] Creek 
 is reached that there is any good natural section of the strata exposed; but here a 
 thin seam of coal with carbonaceous shale is visible on the bank of the creek, ten miles 
 south from Gatton Station, and twelve miles higher up the creek a fine seam of excellent 
 coal crops out in the west bank, just above the upper boundary of Portion No. 9. This 
 seam contains nine feet of workable coal, the top being a seam of coal one foot, then one 
 foot fireclay, six feet of coal, one foot white clay, one foot coal, one foot clay-shale, one 
 foot coal, resting on a thick bed of fireclays and shales. Above the coal, fireclay and 
 thin bands of shale are visible, which are again covered by a mass of basalt, which rises 
 about a thousand feet to the summit of the Great Dividing Range. The coal is nearly 
 horizontal at its outcrop. It is a very hard cannel coal, with cubie fracture, does not 
 cake in coking. Specific gravity, 1°29. 
 
 Volatile in coking A7 
 Fixed carbon nee ae ves a AEE, ns 36 
 Ach Sa ne ft - * a ae ies ie a rf 
 
 100 
 
 “ Coal, Flagstone Creek, near Toowoomba.—tIn the valley of Flagstone Creek, eight 
 miles south-west from Helidon Railway Station,and six miles from Toowoomba, on Parion 
 No. 44, there is a good seam of coal, which has been opened on the south side of the 
 creek by a drive of five or six yards, showing a thickness of fifteen inches; but in the 
 gully, a hundred yards south, the thickness is two feet. The same seam is also exposed 
 on the north side of the valley, but only one foot thick. This coal is moderately hard ; 
 does not cake in coking. Specific gravity, 1°36. 
 
 Volatile in coking 36 
 Fixed carbon se 3 see Bae a a 48 
 Ash En s5e sa ie Paa hss oa at a LG 
 
 100 
 
 “* About two miles to the west of this outcrop of coal a large deposit of rich iron 
 ore shows at the junction of the Carboniferous rocks and the superincumbent basalt, 
 and within a few yards limestone of impure description, apparently a tufa derived from 
 
 the igneous rock. 
 “Coal near from Murphy’s Creek Railway 
 
 Station, many small pieces of coal were found in the bed of a small watercourse, and it 
 is reported that a thin seam of coal has been found in the adjacent valley, but that it is 
 not of sufficient thickness to be of any great value. 
 
 
 
 
 
 * See remarks postea, p. 348, 
 
339 
 
 “ Although there are numerous deep cuttings in the Carboniferous rocks of the 
 Main Range along the line of the Railway between Murphy’s Creek and Highfields, yet 
 no coal-seams have been exposed, though this may in some measure be accounted for by 
 the liue following nearly along the outcrop of a thick bed of sandstone, which has a 
 very gradual rise towards the summit of the Main Range, and passes under the basalt 
 which forms the watershed between the eastern and western waters. 
 
 “Coal at Spring Creek.—Crossing the basaltic tract to the westward, the first 
 point where the Carboniferous strata are visible is at Spring Creek, near the Warwick 
 Railway, six miles west from Toowoomba. Here a thin seam of coal has been cut in 
 sinking a well, and a seam three inches thick, accompanied by black shales and iron- 
 stones, are exposed in the bed of the creek; but the strata being nearly horizontal, they 
 soon pass under the basalt again on all sides, so that there is no great thickness of the 
 sedimentary strata exposed in section.* 
 
 “ Coal, Hodgson’s Oreek.—Six miles W.S.W. from Cambooya Railway Station, in 
 the bed of Hodgson’s Creek, large blocks of coal, some exceeding 1 ewt., have been 
 drifted out of the waterholes; and the Carboniferous shales and soft sandstones are 
 largely exposed on the west side of the creek, extending nearly ten miles to the south- 
 west. The coal is found along the channel of the creek for a distance of two miles, in 
 a condition which indicates that it has only moved a few yards from the original seam. 
 This coal is of excellent quality, being hard and capable of standing carriage and 
 exposure to wet without injury. It does not make good coke. Specific gravity, 1°33. 
 
 Volatile in coking... wn ae fe: oe ee ue we 45 
 Fixed carbon ... a a wae MS ate ne sae wee AZ 
 Ash Ye nae be a “et aoe tae ee ea aso dh 
 
 100 
 
 “ Olifton Coal.—The Clifton Coal Mine is situate two miles beyond the Clifton 
 Railway Station, close to the east side of the line. Two shafts have been sunk, and a 
 bed of coal four to five feet thick is worked at a depth of sixty feet. A second seam of 
 two feet at eighty feet, and a third of one and a half feet at one hundred feet, have been 
 cut in the principal shaft. 
 
 “The Upper Seam, which is the one worked, produces good coal, varying from 
 bright bituminous to dead black oil coal, all being very hard and tough, so that it bears 
 carriage without breaking. It produces a high percentage of gas or oil, according to 
 the mode of treatment. Specific gravity, 1°26 to 1:35. 
 
 Volatile in coking .e ae sas nh as) 
 Fixed carbon Ses NEE aoe os cor SOF oat spe 
 Ash Ae we ae see e sins “Or ie sc son 
 
 100 
 
 ‘*The Second Seam is better suited for coke, as it cokes [cakes ?] in heating. 
 ‘““The Lower Seam is very hard oil coal. Specific gravity, 1°32. 
 
 Volatile in coking 47 
 Fixed carbon ... te ie 1S 2 = Sf > en /) 
 Ash oe 7 aan Ky ee ce a 5ee bo Soo ANS: 
 
 100 
 
 
 
 
 
 * Tt may be remarked that this spot is nearly on the same level as the junction of the basalt and 
 stratified rocks near Highfields, on the east of the Range, so that the bottom of the basalt appears to be 
 pretty level in this locality. Mr. Gregory’s Geological Map shows that the basalt extends many miles further 
 west, and at their western boundary they form no escarpments, but appear to dip under the western members 
 of the Ipswich Formation. (R.L.J.) © 
 
340 
 
 “Situate in an extensive tract of open, nearly level country, the strata seem to 
 have but little inclination, but the general dip seems to be a little to the west. To the 
 eastward the coal rocks are covered by basalt, the edge of which is between the two 
 shafts of the mine, the eastern one being sunk through a considerable thickness of hard 
 blue metal, and at the junction of the igneous and coal rocks a bed of earth was found 
 containing fragments of fossil wood, with the leaves and seed vessels of plants, 
 belonging to a period much more recent than the coal strata.”’ 
 
 The Writer visited the Clifton Colliery, while it was being worked, in 1880, and 
 measured the following section of the Upper Seam :— 
 
 Moh OOOO oHMEe 
 
 — 
 
 Black clay shale ns 
 
 Coal (thickens to 7 inolen 
 
 Grey fireclay .. Ze 
 
 Grey fireclay, with five ita seams ws coal are ots, 
 Coal... ae ees aoe 
 Grey fireclay, with White spots ea a fad Sat seam 
 
 Coal 
 
 Stiff grey clay 
 
 Coal 
 
 Fireclay # da 
 
 According to Mr. Grecras 8 Aeeeracte it may ie surmised that the eastern 
 shaft alone passes through “a considerable thickness”’ of basalt, before cutting the 
 coal. As the dip of the coal is to the west it may be presumed that this mass of basalt 
 (which is unconnected with the main mass of the Toowoomba Range) occupies a local 
 hollow, or possibly an ancient valley. The basalt may even be of a later age than the 
 basalt of the Main Range.* Mr. Gregory continues :— 
 
 “Coal has been found in Clifton Creek to the north-west of Clifton Mine; also in 
 a well sunk through basalt at the head station, while the Carboniferous sandstones and 
 shales are largely developed to the south-west. 
 
 “ Ooal near Allora.—Coal was worked near Allora, about two miles from the 
 Hendon Railway Station, and the coal supplied for use in the locomotives on the 
 Warwick Railway. The seam was not more than two feet thick, and has been 
 abandoned. 
 
 “ Warwick.—The Town of Warwick is situated on an outcrop of the Carboniferous 
 sandstone, containing great quantities of fossil wood, changed mostly to iron ore; and 
 to the east and north of the town the soft shales indicate the probability of coal existing 
 at a small depth, small fragments of it being found five miles to the south-east of the 
 town; also in a well on the Agricultural Reserve. 
 
 “Coal at Farm Creek. or Farm Creek, fourteen miles east from Warwick, the 
 outcrop of a large seam has been worked for the supply of the steam mills. 
 
 “ Character of the Coal, §c.—The general character of the coals found between 
 Walloon and Warwick is that of cannel coal. It does not cake in coking, gives a 
 high percentage of gas, or oil and paraffin, according to its treatment at a high or low 
 temperature. Its hardness renders it very suitable for export. It burns very freely, 
 and leaves a soft, white ash. From the small proportion of fixed carbon, and its not 
 caking, it does not produce good coke, but a charred coal, which, however, burns well; 
 consequently it is not well adapted for blast furnaces, though well suited for rever- 
 beratory furnaces. As a steam coal it is best suited for stationary or marine engines, 
 the strong blast of locomotives being apt to blow it through the tubes. It is a very 
 high-class household coal. 
 
 ~ : 
 CWO NW wm HOF 
 
 bho 
 o 
 oO 
 
 
 
 * Vide my Colleague’s remarks on the Plant-remains referred to by Mr. Gregory. (R.Z.J.) 
 
341 
 
 “Tn the Ipswich division the coals are bituminous, coking well. The proportion 
 of gas being small and the fixed carbon large, they are suited for forges and blast 
 furnaces ; are good steam coal when not broken too small, but are so friable as not to 
 bear carriage well, and suffer from exposure to wet, so that the harder varieties, though 
 containing most ash, are found in practice to be most economical, in consequence of the 
 smaller proportion of waste. 
 
 “Tn both districts the coal is associated with ironstone bands and beds of boulders 
 consisting of concretions of oxide of iron, which have replaced fragments of fossil 
 
 wood. 
 ANALYSES OF Coats In IpswicH ForwAtTIon. 
 
 
 
 
 
 
 
 
 
 
 
 Mine or Localit es gs ere Ash Cok ee rd 
 
 peek ot Carbon. re pe Coke. Coke. 
 
 Tivoli Mine, North Ipswich ... es ata'| ) LEME 66'4 6-9 73°3 90°6 9°4, 
 Eastwood Mine, North Ipswich ee ORO 63:0 12:0 750 84-0 16°0 
 Thompson’s Mine, Bundamba ... sos ans Sle7 62°3 6:0 68°3 91:2 88 
 Goodna Mine ... 5 S00 iss see 28'8 62°2 9:0 71:2 874 12°6 
 New Mine, near Tivoli Mine ... at Si) 1307S 61:0 82 69°2 88:2 11°8 
 Thomas’s Mine, Bundamba ... aa ae 29'8 59°2 11:0 702 84:3 1537 
 Aberdare Mine, Goodna : spa) site! 572 14-0 71-2 80°3 19°7 
 Blond and Wright’s Mine, } North Ipswich tn 20'S 564: 17-4 73°38 76°4: 23°6 
 Lyons’ Shaft, Moggill oat : ey 38°2 51:0 108 61'8 82°6 17-4 
 Brisbane River Seam, Rocky Crossing ree, 220 50°9 271 78:0 65°3 34:7 
 Flagstone Creek, Helidon ae at ae 36°3 47-4 16°3 63°7 744, 25°6 
 Blackfellow’s Creek, West Moreton ... Se dee oe 45°6 12-0 57°6 70°2 20°8 
 Hodgson’s Creek, Darling Downs _... we | 4a 42°6 12°7 55°3 770 23:0 
 Clifton Mine, Darling Downs eo Ss fe A7°6 42-2 10-2 52°4 80°5 19°5 
 Walloon, West Moreton % ey | 47:0 36°0 17.0 53'0 67:9 82°1 
 Murphy’ s Seam, Kedron Brook | = ko O 33°6 50.4 84°0 30°0 70'0 
 
 
 
 
 
 
 
 
 
 For CoMPARISON. 
 
 
 
 
 
 Miva Seam, Mary River ¥S a ieee 2o'G 61:0 15-4 76'4 80°0 200 
 Pine Creek Seam, Burnett River... sa 34°3 575 62 63°7 90°3 7 
 Waratah, New South Wales .... ks a 31:0 62°5 65 69:0 90°6 974,” 
 
 
 
 
 
 In another Report,* Mr. Gregory notes the presence of coal ‘in the bed of the 
 Condamine, about two miles south of the Railway line, forty miles beyond Dalby,” about 
 the 193-mile peg, and adds, “there are several thin seams of good cannel coal which 
 would be available for use in locomotive engines. The coal isa hard gas coal, which 
 does not cake. It bears carriage and exposure to weather with but little injury, but it 
 burns very quickly and has a high percentage of ash, and consequently will not do an 
 equal amount of work per ton as the softer coal from the Ipswich mines.” 
 
 Mr. William Fryar, Inspector of Mines, has kindly given me the following 
 details of sections of the various Ipswich Coal Seams :— 
 
 Aberdare.— 
 
 Ft. In. 
 Codlman see ae An U As Ee if ler Re) 
 Band... owe oe df he ae Be Orel 
 Coal” ... ah oe a il 
 Band ... he 5 ied: 
 Coai-= .: are ae Bos oe ae 58 Age “By sg) 
 Band ... a ae sa ee “oe if oh nf ree Oe 
 
 
 
 
 
 * Report on the Search for Coal between Dalby and Roma. Brisbane: by Author.ty : 1879, 
 
342 
 
 Ft. in. 
 Coate., Ovil 
 Band 0 4 
 Coal , 1 4 
 Bands of clay and worthless eee Le 
 Coal , 1S i7e 
 Bane O O08 
 Coal ... Oma) 
 Band 0 2 
 Coal . 3 6 
 
 The Hine is 13° to S. 74° W. The ere seam (shone Six Peay is first worked, 
 after which the “tops” are taken down. In the new tunnel the dip is 12° to west and 
 south of shaft 20°.* 
 
 Mount Pleasant.—This is a seam worked by Messrs. Stafford and by the Bore- 
 hole Company in adjoining land. It is probably one of the seams being worked (by 
 Messrs. Green and Jones), or cropping out in Mr. Allen’s property adjoining. The 
 dip is 1 in 3 W. 10° S. 
 
 Ft. in. 
 Coal , RE 0 8 
 Titernittent and. of rorsiene bold eran 0 8 
 Coalan 1 0 
 Band... Oo 1 
 Coal . Jano 
 
 Cn in PES 8 hadones ehgeh oy Ean ae nroperty Se seams of coal are 
 
 worked by Messrs. Green and Jones, of which the following is an approximate 
 section :— 
 
 Ft. int. 
 Seam (h) _... im See eae He iris uae Me ae 4 0 
 Strata ea 45 Sire ‘es a oe Ae eM) 
 Seam (g) with two oll Bene 5 ee ak war + ea 3 0 
 Strata ee ae st ne re NM) 
 Seam (f), coarse, only ee eet pee REED a oe = 8 0 
 Strata oe vad ae a Sa Sc ee ie he oka 
 Seam (e)... fie aie oe ss - on nad eee 2 6 
 Strata ae see es “i -— = as ae 6020 
 Seam (d)... a sis oy bei ei en Ss we ecu 
 Strata ae ves aoe fh gc2 is ts Fae pee ty OW 
 Seam (ce)... ~~ at ves ve as fe ws x OG 
 Strata a Be 7 es te ae ee ee or LDU Ray 
 Seam (6)... ia os ae sie ee Ses ea ona 0 0 
 Strata te “a3, SURO 
 
 Seams (c) “siti Gye crop ane in the pediec mick a ie of 30° to 33° W. 
 
 Scarborough’s Seam is four feet in thickness, with three small variable bands, 
 irregular in thickness and position. It is worked at the Day Dawn Mine, Parish of 
 Goodna. 
 
 Stafford’s Seam (which, however, is not the same worked by Messrs. Stafford) 
 adjoins Scarborough’s Seam. Its thickness varies from two feet six inches to four 
 feet. It has many small dislocations, and usually two thin bands. 
 
 The Ebbw Vale Seam, near Dinmore, has a thickness of three feet four 
 
 inches, with a band of ironstone boulders in the middle, It dips at 10° to 15° to 
 E. 10° N. 
 
 * T cannot be certain whether this is the same seam as that referred to by Mr. Gregory in the 
 heading of ‘‘Thomas’s New Coal Mine,” which is called the Aberdareby the Rey. Mr, Tenison Woods. (R.Z.J.) 
 
843 
 
 Braeside.—The Braeside Seam is about three feet thick, and has several small 
 bands of clay. The dip, which, however, varies considerably, averages 15° to 
 the S.W. 
 
 Bundanba New Chum.—This seam is three feet to three feet nine inches in 
 thickness. It dips in the No. 4 Tunnel to 8. 10° E. at 10°. 
 
 Bundanba.—This seam is met with in New Chum Shaft beneath a thicker and 
 coarser seam. It is four feet six inches in thickness, and is free of bands, although an 
 occasional boulder is met with. It dips at 1 in 9 to south-west. 
 
 Bundanba New Pit.—This seam is four feet thick, with an intermittent band. 
 It dips at 8° to S. 35° W. 
 
 Waterstown.—The seam at present worked is three feet two inches thick, with 
 several small bands. 
 
 Erskine’s Seam, Ross End.—This seam is worked from a shaft one hundred and 
 sixty feet deep. It lies thirty-two feet below the Ross End Seam. The strata dip at 
 18° to S. 10° E. A six-inch band divides an upper seam of coal, two feet three inches 
 in thickness, from a lower seam of eighteen inches. 
 
 Walloon.—The seam, worked by the Walloon Coal Company, dips at 13° to W. 
 10° S. The following is a section of the seam :— 
 
 Ft. in 
 Coat 3s. Teo 
 Clay band 0 5 
 Coals. i. 0 3 
 Clay band O 4 
 Coals. O=5 
 Clay band G1 
 Goalerr, <. 0 8 
 Clay band Ol 
 Coal IO 
 
 Eclipse.—This seam, which is worked by Mr. John Wright, is a pretty clean 
 coal, five feet six inches in thickness. 
 
 In the paragraph on “ Coal near Rosewood Station,” above quoted, Mr. Gregory 
 speaks of the coal-bearing strata resting on “limestone containing corals of the 
 mountain limestone series.’ This, of course, if correct, would be important evidence 
 as to the ave of the [pswich Coal Measures, and [ sent the late Mr. James Smith to the 
 locality in June, 1890, with instructions to search the district thoroughly. Mr. Smith 
 reported that he had examined all the sections in the neighbourhood, without finding 
 any “ Mountain Limestone.’ He found, however, in the bed of a creek, about a mile 
 west of the Farmers’ State School, numerous boulders of a peculiar ironstone, exactly 
 similar to that found at Laurence’s Homestead, Stewart’s Creek, Rockhampton, and 
 containing a similar assemblage of fossils, and, in addition, some concretions which my 
 Colleague has recognised as very similar in appearance to the genus Apiocrinus. In the 
 Map accompanying Mr. Smith’s Report, he marked Sections 2v, 66, and 102, Parish of 
 Grandchester, as the locality where these fossils occurred. 
 
 Mihi.—This seam is worked by the proprietors of the Eclipse, and has the 
 following section :— 
 
 Ft. in 
 Coal at a Sai sae sf he sic oy, te pa AO 
 BAG Bert. oat aa = ae se an ah ie ee Ae 
 OGLE nc. BA iy Pk aa ade we cfay Mes big oO 
 Band... ae Pan at ate ie oe ee af Oe ua 
 Cogtiann. Aa mn a eek =i Sn Nee 2 fae ek 
 
344 
 
 In his Pamphlet on “The Coal Resources of Queensland,’’* the late Rey. J. E. 
 Tenison Woods gave the following particulars :— 
 
 “Waterstown Mine.—This is a colliery which is being worked by two or three shafts, 
 all on the north side of the Bremer, and very close to its banks, and where it is navigable 
 for small craft. There is a shaft upon the Garden Seam, which is about seven feet thick, 
 and crops out upon the surface. It has a dip of usually 1 in 5 8. 15’ 20° E. The coal 
 has a short fracture, breaks into small cubes, soils the fingers, and is full of bright 
 bituminous streaks. Of the coal from this mine Mr. A. C. Gregory reports :—‘‘ The coal 
 is a fairly hard coal, cokes well, and ig a good steam coal.” The following is the 
 analysis :— 
 
 Fixed carbon sph “8 See seh 508 ed te ... 62:0 
 Volatile hydrocarbons “ie sot coe cork Gee aa os 2p2 
 ATi ar ae ise a Ji aa ae Sic Poe say HRS) 
 
 100°0 
 
 “ Above the seam there is about four and a-half feet of splendid fireclay. The seams 
 connected with the Waterstown Coal Field are the Edina, Eclipse, Tivoli, and Old Tivoli. 
 The Bell Seam, which is about a mile from the Garden Seam, and belonging to the same 
 proprietor (Mr. Moffatt), is about three and a-half feet thick. It seems a more compact 
 coal than the last, and is a first-class coal for steam, gas, and coaking. It is worked by a 
 drive like the Garden Seam, about two hundred yards long, and dipping 16°, which is the 
 dip of the seam, the direction being 8. 15° E. There is supposed to be a fault between 
 this seam and the Garden Seam. A seam which crops out near the latter, and which 
 has thinned out, may be the same. Its true position is supposed to be one hundred and 
 fifty feet below the Garden Seam. <A new drive has been made on the outcrop (sup- 
 posed) of the Garden Seam, about a quarter of a mile from the pit referred to last. 
 It is extremely good coal, with scarcely any partings in the seam. 
 
 “On this property there is a large coking kiln which has been in operation some 
 eight years, and during which some four or five thousand tons of coke have been turned 
 out. The coke is made from the very fine slack and dust. It is of splendid quality, 
 and is exported to Rockhampton, Maryborough, and even Melbourne, to the iron 
 foundries. It sells in Brisbane at about £1 17s. 6d. per ton. 
 
 “ Rossend.—The Rossend Mine (Lindsay’s) adjoins this property. It is worked by 
 one shaft, to the extent of about 20 tons daily, on what is supposed to be the Bell Seam. 
 
 “ Tivoli.—The Tivoli was until lately extensively worked, as its proprietor had the 
 railway contract, and was able, by a short tramway with a steep incline and shoot, to 
 load al] the lighters on the river. He has now the contract for the Australasian Steam 
 Navigation Co., and finds it more convenient to work on another seam on the south side 
 of the river. On the Tivoli Mine there is one shaft and three seams. The Eclipse 
 Mine works on one seam of the old or original Tivoli.” 
 
 Of the portion of the field above referred to, the late Mr. Tenison Woods further 
 remarked :—‘‘ There are probably five different seams at present worked. These are: 
 (1) Garden Coal; (2) Edina Coal; (3) Tivoli; (4) Old Tivoli; (5) Bell Coal. No 
 
 data can be given as to the distances of these seams from one another. 
 
 * 8vo. Brisbane, 1883. Attention should have been called in a previous chapter to two pamphlets by the 
 late Rev. J. E. T. Woods on the Burrum and Burnett Districts, viz., ‘‘ Lecture on the Burrum Coal Field ” 
 (pp. 12, 8vo., Maryborough, 1881) and ‘‘The Carboniferous Rocks of the Lower Burnett: A Lecture 
 delivered at Bundaberg on Friday, May 20th, 1881” (pp. 4, 8vo., Bundaberg, 1881). 
 
 + Mr. Gulland believes.the position of the Waterstown Seam to be five hundred feet above the Tivoli 
 Seam. (R.L.J.) 
 
 + The manager of the Toowoomba Gasworks informed me, in 1880, that the Waterstown coal yielded at 
 the Works 9,200 cubic feet of gas, (R.L.J.) 
 
345 
 
 “ New Chum Shaft.—At Bundanba there is a colliery worked by a pit (New Chum 
 Shaft), the property of Mr. Gulland. The shaft is about two hundred and twenty feet 
 deep, tapping two seams, the lower one of which only is worked. The latter shows in 
 all about twenty-seven feet of carbonaceous matter, butrof this four feet to four feet 
 eight inches is good clean coal, without any partings or shale. The dip is about 1 in 9, 
 a little east of south. It is a good, firm, shining coal, with much mother-of-coal in the 
 partings ; yet it does not soil the fingers as much as other coals on this field. It is 
 entirely sold for steam purposes, with the exception of the slack, which finds a ready 
 market for smith’s work.* 
 
 “ Braeside.—The Braeside Shaft is a mine of Mr. Lindsay’s, rather over a mile 
 from the New Chum. The workings are a drive along the seam, which is three feet 
 thick. The coal is very similar to the last. The drive is two hundred and eighty yards 
 long. There is another shaft close by, sixty yards deep, 0a a second seam of a superior 
 coal. 
 
 “ Southern Coalfields —All around Pine Mountain and Peak Mountain (‘“ Flinder’s 
 Peak” on maps), and for a distance of many miles to the south and west, there are 
 outcrops of coal. ; 
 
 “Walloon Coal.—About six miles west of Ipswich is the Walloon Colliery. The 
 seams are three in number. The first erops out on the surface, with a dip, to the south- 
 west, of lin 9. The seam is remarkably compact,, with about four and a-half feet of coal. 
 The second seam is fifty feet below, with five feet six inches of good coal. A third 
 seam is found forty feet deeper, about five feet thick. This coal differs completely 
 from all the other seams found around Ipswich.¢ It is perfectly clean and compact, 
 and does not soil the hands. It is not brittle, so that there is little or no slack in the 
 handling. It has a smooth, bright, jet-like lustre, with bright bituminous streaks. As 
 a gas coal it has no equal in the Colony, and also as a household coal. The average of a 
 number of proximate analysis would give a percentage of— 
 
 Fixed carbons ... re yes “hf 4c on wt ws * 90 
 Hydrocarbons aa Gas oA 9a see pale aAv ~3 40 
 Ash oo ES. aoe ve ag ie 56 mcd Ade ee 
 Loss, moisture, &c. < sas ee wie ni sue se ars. 
 
 100 
 
 “Some specimens do not coke well; others yield about 50 per cent., bright and well 
 swollen up. The seam is worked by @ drive which runs ina south-westerly direction 
 for about one hundred and thirty-two yards, with a dip of about lin 7. The drive, at 
 the present, opens into three levels, the lowest of which is about seventy-five feet from 
 the surface. At this level a magnificent seam of coal, five feet thick on the clear, is 
 met with, and is intersected with a layer of fireclay of about three inches in thickness. 
 
 “A coal seam, known as ‘ Morgan’s,’ crops out about seven miles north-north- 
 east of Warwick.’’§ 
 
 J. 
 
 * The two seams, I was informed by Mr. Gulland, the proprietor, are separated by two hundred feet 
 of shale and sandstone, (2.L.J.) 
 
 + It is not the seam near Walloon referred to by Mr. Gregory. (R.Z..J.) 
 
 + This is, I presume, what is now known as Rea’s, or the Caledonian Seam. (A. LZ...) 
 
 § Some good sections of seams and analyses of coal will be found.in a pamphlet, ‘‘ Queensland, 
 Australia; its Territory, Climate, and Products” (pp. 117, plates, &c., Svo., London, n.d.), issued by the 
 late Mr. Richard Daintree, C.M.G., when Agent-General in London, (See pp. 77-80). (R.A. Junr.) 
 
 
 
 
 
CHAPTER XXVII. 
 
 THE TRIAS-JURA SYSTEM—continued. 
 
 THE IPSWICH FORMATION (UPPER TRIAS-JURA), IN THE TYPE DISTRICT —continued. 
 
 The outcrop of a nine-inch seam of poor shaly coal is seen in the railway cutting 
 (Brisbane Valley Branch) south of the bend of the Brisbane River, south-east of 
 Lowood Station. It lies beneath a thick bed of sandstone, and overlies a considerable 
 thickness of soft sandy shales and thin bedded sandstones. The strata undulate 
 gently, but dip, if anything, to the east. 
 
 A well in Portion 473 (D. Kennally’s), Parish of Walloon, gives the following 
 section :— 
 
 Feet. 
 Surface (sand and boulders of basalt, &c.) ee ee rs ye 50 
 Decomposed sandstone a ore be nis 10 
 Brown ferrugino-calcareous eandatone! WwW ith planta ie eee cs 10 
 Coal... ie af ns ar Be ah 3 
 Fine conglomerate and grey eaudstons ee ee ae ae a 67 
 140 
 
 The dip of the strata is about 1 in 12 to the east. The water in the well is 
 rather salt. 
 
 In the whole of the Rosewood District, within a circle of five miles radius of 
 the Town of Marburg, the strata consist, for the most part, of sandstones and shales, 
 with beds of red hematite nodules; but there are very few continuous sections. A 
 landslip, which took place owing to the heavy rains of the beginning of the year 1890, 
 exposed a two feet bed of limestone on Portion 518 (Gadischki’s), Parish of Walloon. 
 The strata are, on the whole, nearly horizontal, and are surmounted by isolated 
 cappings of basalt, forming the higher hills of the district. 
 
 A series of very remarkable landslips took place in the Rosewood Scrub District 
 in the beginning of 1890, following on a wet season of unprecedented severity. In this 
 district the primeval “scrub” or jungle had been cleared, and the land settled and 
 cultivated by a colony of German farmers. The great depth of soil, which was often of 
 a clayey nature, had been saturated with water till it became semi-liquid mud, and 
 travelled down the slopes of the hills. At least a hundred acres of land “travelled”’ 
 more or less on different farms. In some cases the lateral movement was as much as - 
 a hundred feet. The removal of the scrub was one of the most powerful predisposing 
 causes of the ruinous havoc. The superficial layer of soil, though held together for a 
 time’by the roots of the growing crops, was finally rent asunder into huge crevices like 
 those on a glacier. 
 
 After the landslips had taken place, it was constantly to be remarked that springs 
 and gullies, which before the floods had been sources of fresh, or nearly fresh water, 
 had become so highly charged with saline solutions as to be unfit for drinking. This 
 could only mean that the water which in ordinary seasons penetrated the crust of the 
 earth percolated only through strata from which the soluble salts had been already 
 
347 
 
 removed, while in a very wet season strata still retaining undissolved salts were washed 
 by the water. Indeed the quality of the water met with in most of the deep shafts in 
 the Ipswich Coal Field shows that the strata are highly charged with salts. 
 
 The Ipswich Coal Measures fossils are exclusively the remains of land vege- 
 tation or of marsh or river mollusca, with the exception of the Insect-remains 
 afterwards referred to, while on the other hand the strata of the Rolling Downs 
 teem with the remains of marine animal life. Even the limestones of the Ipswich 
 Formation have yielded no trace of marine organisms. We are forced, from this 
 circumstance, as well as from the saltness of the strata of the Ipswich Formation, 
 to conjecture that the latter was for the most part deposited in an inland lake. It 
 must be remembered that some lakes, especially such as have no outlet, are much salter 
 than the ocean. ; 
 
 My Colleague casually examined the beautiful Collection of Plants made by Mr. 
 J. H. Simmonds, of Brisbane, in August, 1890. Amongst the specimens he recognised 
 several Insect-remains and one very beautiful Hstheria. These have since been described 
 in detail, and it may be well for me to point out that they certainly, to some extent, bear 
 out the above opinions. 
 
 The output of the Ipswich Coal Field from 1860 to 1890, inclusive, is estimated 
 at 2,339,013 tons of coal, valued at £1,048,649. It is possible, however, that between 
 1860 and 1883 a small proportion of the output credited to Ipswich was produced at 
 the Burrum. On the other hand, it is more than likely that a portion of the coal from 
 Clifton may not have been included in the returns, as the products of this colliery 
 were to some extent consumed locally. 
 
 YIELD OF IpSwicH CoAL FIELD. 
 
 
 
 
 
 Year. Tons of Coal Value. 
 Raised. £ 
 
 1860 to 1883 ... Sonn Even see ... 814,407 wee 414,368 
 1883 i ba a ro ... 98,310 a 49,114 
 1884 a6 oh a ves we 114,577 aa 56,475 
 1885 ain os bee = .» 180,744 ant 71,258 
 1886 vee ‘xs ae ee ... 189,608 ase 72,054 
 1887 ee tes wee ose .. 193,286 use 71,851 
 1888 ay vee ee oe 254,778 nas 97,851 
 1889 at vee wee 0 ... . 217,240 see 95,202 
 1890 Se E ase wes ... 276,063 = 120,476 
 Totals ce “ss 2,339,013 ne 1,048,649 
 
 Of the Jimbour coal the Hon, A. C. Gregory reports as follows* :— 
 
 “At the Dingo Point Well the shaft has been sunk through seventy-six feet of 
 surface soil, then three and a-half feet of impure coal which would wake a safe roof, 
 when a seam of coal eight feet thick, but with five bands of shale having an aggregate 
 of one foot, leaving seven feet of workable coal, under which there is thirteen feet of 
 fireclay and shale, and a second coal-seam four feet thick, with three thin partings of 
 clay. But the lower seam, in consequence of water in the shaft, could not be fully 
 examined. 
 
 “The dip of the coal, so far as could be ascertained in the small space of the 
 
 shaft, is about 3° to the 8.8.E., in which direction a dyke of basalt shows on the surface 
 about a quarter of a mile distant. 
 
 
 
 * Brisbane: Watson, Ferguson, and Co, ; 1884. 
 
348 
 
 “The country being nearly level, and strata horizontal, there is reason to suppose 
 that no great disturbance of the coal-seams exists, more especially as on the line of strike 
 to the west, coal has been struck in a well some two and a-half miles distant, and 
 seven miles to the northward, at the Jimbour Station; the seam of coal worked there 
 has every appearance of being identical with that at ‘ Dingo Point.’ 
 
 “The quality of the coal is that known as ‘free burning long flame’ or ‘ cannel’ 
 coal. It is hard and brilliant in fracture, does not soil the hands, and will stand 
 exposure to weather or rough carriage without injury or loss by waste. It ignites with 
 great facility, burns freely with long flame and comparatively little smoke; it does not 
 coke, but burns to white, heavy ash without any cinder. As a steam coal it comes 
 closely up to the average of the Ipswich coal now in use on the railway in regard to the 
 work done per ton, but it has a great advantage in its superior hardness and weather- 
 resisting qualities, while the Ipswich coals are so tender that it is difficult to prevent 
 their wholly falling into ‘slack.’ . 
 
 “The economic value as a gas coal is about double the average of the Ipswich 
 coals. 
 
 “As a household coal its qualities are excellent, being very clean, and burning 
 freely even in small quantities. 
 
 “ Apart from the value of the Jimbour coal as fuel, it has a higher prospective 
 value as a source of paraffin and illuminating oils, giving sixteen and three-quarter per 
 cent. of crude petroleum, or about thirty-seven gallons per ton of coal. 
 
 “he accompanying statement of the particulars of the testing of the coal for 
 economic purposes gives the more important features of its quality. The samples in 
 each case were not picked, but taken from the average of the portion of the seam 
 represented, as a commercial average in ordinarily working the mine :— 
 
 “DETAILS OF Tests FoR Economic VaLur oF Coal FROM JIMBOUR. 
 “The coal being burnt in a 2-H.P. vertical engine, the feed water at 78° F. Steam got up with 
 wood, and fire withdrawn and coal lighted. Steam 20 1b. 
 
 Jimbour Coal. 
 
 : Lb. 
 
 No. 1 Coal, 12 inches (Top of seam)— 
 
 Coal burnt 5 5 we ate i. 100 
 
 Water evaporated... vis ma a Ms a ... 498 
 
 PAS lr uae ee gl tee bc “iad ean nee Bast le: 
 No, 2 Coal, 15 inches— ; 
 
 Coal burnt... ai of, ee ne fe, aie ee LOO 
 
 Water evaporated... ane Se ie sa AB aon aye) 
 
 IMA, gos wes i oh Se re Pah tea ee ALO 
 No. 3 Coal, 94 inches— 
 
 Coal burnt... fe ies Ave sive we Mi LOG 
 
 Water evaporated ... vas re sts ae hes i 407 
 
 Aces Le: aa wee ac ane re sae yee ike} 
 No. 4 Coal, 24 inches— 
 
 Coal burnt... <n re Bas ee es 560 ae LOO 
 
 Water evaporated... 56 vet ie rc ie = 498 
 
 FAs ies ie viae aoe tee oe an a Neue ee) 
 No. 5 Coal, 15 inches— 
 
 Coal burnt... de a6 nan sats ae so =, 200 
 
 Water evaporated... nee =e aS, aos se RO 
 
 Agha s. ose de siaks vee a ea ia a a20 
 
349 
 
 Ipswich Coals. 
 
 Lb. 
 
 Waterstown, Ipswich— 
 
 Coal burnt... ae a io On eh nae sa. KG.) 
 
 Water evaporated... a ves aC are ats ». 499 
 
 ‘Ash + 4,2 ne ss m3 ee eee ee i tgp 18 
 Thomas’, Bundanba— 
 
 Coal burnt... Ars 1 ake 28 a Tie eee LOO 
 
 Water evaporated... sie he aa ee en eeto07 
 
 cA aha is vir To: oe ne ae S00 ee LD 
 Walloon Coal— 
 
 Coal burnt... oe nae ot ade aa aie ere OO 
 
 Water evaporated ... or exe Me red 5 we 457 
 
 Ash ... ees ae ae aa a8 vet re ae LO 
 Tivoli Coal, best— 
 
 Coal burnt... mc aoe ae a yea wa son OD 
 
 Water evaporated ... ee ae as ans Soe vw. 561 
 
 PACS ieee ane Ae sion oie ade ee see fe LO 
 Tivoli Coal, second— 
 
 Coal burnt... nae Soe Ac ae bc ane sc AMONG, 
 
 Water evaporated ... sige a ae ‘is ae <6 499 
 
 IAQ aap 5 SA ven Fc a set Wee me a Pe 
 
 New South Wales Coals. 
 
 “ Waratah,’ Newcastle, New South Wales— 
 
 Cealburnt ... * 08 ne tas at wee Bee ane aoe) 
 
 Water evaporated... ane oe fa a ne oo AO: 
 
 Ashi “6 ie aes se He Mi ate tee 73 
 
 “rst oF AVERAGE FROM ALL PARTS OF THE JIMBOUR CoAL SEAM, FOR O11, &c. 
 lb. per cent. 
 
 Coal distilled in retort << see ane soo 10S ee 100 
 Coke remaining in retort... ae aA sop od he 47 
 Oil, 8.G. 0°975 isa sai Pay, an fae L2 a 16°7 
 Ammonia, Water... aie oat see see ay 76 
 Uncondensed Gas, &e. o a ae vee 205 er 28°5 
 
 “The coal does not coke, and is not suited for coke or smiths’ forges and similar 
 work. Average specific gravity, 1°275.” 
 
 The output of the Jimbour Coal Field is given in the “Annual Report of the 
 Department of Mines”’ for 1885 as 2,040 tons, valued at £1,020. 
 
 The exact line of demarcation between the Ipswich and Rolling Downs Forma- 
 tions has not yet been satisfactorily traced, but there is reason to believe that the former 
 gradually passes upward into the latter on the inland side of a line running north- 
 westward from the heads of the Macintyre to Dulacca Railway Station. Beyond that 
 line the presence of marine Cephalopoda and Pelecypoda sharply define the transi- 
 tion from inland or freshwater to marine conditions. 
 
 Whether the Ipswich Coal Field can be traced beneath any large area of the 
 Rolling Downs Formation is a question which may in the next century assume an impor- 
 tance comparable to that of the presence of coal beneath the Cretaceous rocks of Kent. 
 So far, none, or only one or two of the deep bores for artesian water in the west have 
 reached the bottom of the Rolling Downs Formation. The latter, in the north and west, 
 directly overlies the older schists, so that the absence of the Ipswich Formation there is 
 certain. Its absence may be due rather to an upheaval at the end of the Ipswich Period 
 than to the thinning out of the strata. 
 
350 
 BASALT AND OTHER IGNEOUS ROCKS ASSOCIATED WITH THE IPSWICH 
 FORMATION. 
 
 The relation of the basalt of Mount Tambourine to the Ipswich Formation is well 
 shown by the remarks made by Mr. Rands on the junction-line between the schists and 
 Ipswich Formation. The straight junction-line between the two formations can hardly 
 bé anything else than a line of fault, and the basalt overlies not only the portion of the 
 Tpswich Beds seen in that neighbourhood but also the schists and the still more recent 
 fault. To the south and east the basalt directly overlies the schists in the Macpherson 
 Range, and in outlying patches between that range and Burleigh Heads. 
 
 In the Toowoomba Range the bedded basalt overlies a portion of the Ipswich 
 Formation, and presents a succession of steep escarpments to the east. Outlying patches 
 of basalt, overlying members of the Ipswich Formation, apparently on a lower horizon, 
 form ‘The Knobby”’’ and other hills in the Rosewood Scrub. To the west of the Too- 
 woomba Range, the basalt beds form no escarpments, but sink beneath an accumulation 
 of strata, separated indeed from the Ipswich Coal Measures of the other side of the range 
 by an unconformability and an immense outburst of basaltic lavas, but still apparently 
 belonging to the same series and characterised by the same fossils. To this western 
 series belong the Coalfields of Jimbour and Clifton, which are, therefore, on a higher 
 horizon than the Ipswich Coal Field proper. 
 
 The basaltic lava-flows, therefore, were poured out after the deposition and 
 partial upheaval of a great part of the Ipswich Coal Measures, and were subsequently 
 covered by a considerable thickness of strata still belonging to the period grouped, from 
 lithological similarity and similarity of organic remains, as the Ipswich Formation. In 
 short, they are contemporaneous with the Ipswich Formation. 
 
 It is a mistake to suppose that the whole of the basalts comprised within the area 
 occupied by the Ipswich Formation form one continuous series. In the neighbourhood 
 of Ipswich, masses of basalt are clearly interbedded with the stratified rocks. (See 
 Plate 49, fig. 1.) At Clifton and elsewhere masses of basalt appear to occupy local 
 hollows in the stratified rocks. 
 
 My. Rands describes the basalt of Tambourine Mountain as amygdaloidal on its 
 upper surface, as including large patches of obsidian and pitchstone, as being “ generally 
 full of olivine crystals,’ and as being occasionally columnar, the hexagonal pillars being 
 often twenty feet in length and three to four feet in diameter. 
 
 Mr. Rands describes * a mass of trachytes containing beautifully developed 
 crystals of sanidine felspar, as occurring in railway cuttings between Logan Village and 
 Beaudesert, near Walton Station. It appears to have come up through the Ipswich 
 Coal Measures, and to have flowed over a portion of them, as shown in the Section PI. 49, 
 fig. 8. A similar rock is described as occurring about a mile west of Walton Station, 
 “apparently interbedded with the Ipswich Beds.’ Mr. Rands classes these trachytes in 
 his Albert and Logan Report as ‘“ Older Volcanic” —7.e., older than the Toowoomba and 
 Tambourine basalt—and it appears to me on insufficient grounds. There can be little 
 doubt, from the Geological Map attached to the Report, that the trachytes occur among 
 strata, which are on a higher horizon in the Ipswich Formation than those on which the 
 basalt of the Tambourine Mountain rests, and, whether interbedded or intrusive, they 
 are not necessarily older, and may even be newer. 
 
 Referring to the basalt, Mr. A. C. Gregory says + that “the carbonaceous sand- 
 stones and black shales are visible in the ravines within a quarter of a mile of the highest 
 
 
 
 * Report on Logan and Albert, 1889, 
 + Report on the Coal Deposits of the West Moreton and Darling Downs Districts. Brisbane: by 
 Authority: 1876, 
 
351 
 
 part of the Great Dividing Range, but are then covered by basalt from a hundred to 
 eight hundred feet in thickness, and having a minimum breadth of seven miles, beyond 
 which the sandstones emerge in horizontal beds, so closely resembling those on the 
 eastern side that it may be inferred that they are only interrupted along the fissures 
 through which the basalt has been erupted.” It will be observed that Mr. Gregory says 
 nothing of the reappearance of the basaltic escarpments on the western side of the 
 Range. 
 
 Our ideas of the relation of the basalt to the Ipswich and other Formations are 
 shown by the Diagram-Section, Plate 49, fig. 2. 
 
 LIFE OF THE PERIOD. 
 
 The following is my Colleague’s List of Fossils from the type district of the 
 Ipswich Formation :— 
 
 Kingdom—PuLantm. 
 Section—CRrYPTOGAMTA. 
 Class—A COTYLEDONES. 
 Order—CaLAMARIER. 
 Family—EQvISsETACE®. 
 Genus—Equiserum, Linneeus. 
 Equisetum rotiferum, Ten. Woods. 
 Loe. Walloon. Also occurs at Stewart’s Creek, Rockhampton. 
 Equisetum ? latum, Ten. Woods. 
 Loe. Esk Valley. Also occurs at Rosewood, Rockhampton. 
 
 Family—Scn1zonevRe®. 
 Genus—PHYLLOTHECA, Brongniart. 
 Phyllotheca carnosa, Ten. Woods. 
 Loe. Walloon. 
 Phyllotheca, sp ind. (Pl. 42, f. 1.) 
 Loc. Bundanba. 
 
 Family—CaLaMitE®. 
 Genus—VERTEBRARIA (Royle), McCoy. 
 Vertebraria equiseti, Ten. Woods. 
 Loc. Tivoli. 
 
 Order —FI1LIcEs. 
 Family—SPHENOPTERID®. 
 Genus—SPHENOPTERIS, Brongniart. 
 Sphenopteris Baileyana, Ten. Woods. 
 Loc. Rosewood, near Ipswich. 
 
 Genus—TRICHOMANITES, Goeppert. 
 Trichomanites laxum, Ten. Woods. ? 
 Loc. Rosewood, near Ipswich. Occurs also at Burrum 
 Trichomanites spinifolia, Ten. Woods. 
 Loc. Rosewood, near Ipswich ; and Redbank, north of Laidley. 
 Trichomanites elongata, Carruthers, sp. 
 Loe. Tivoli and Aberdare Mines; and Rosewood, near Ipswich. 
 
 Family—NEUROPTERID®. 
 Genus—THINNFELDIA, Ettingshausen. 
 Thinnfeldia odontopteroides, Morris. 
 Loc. New Chum, Bundanba; Aberdare; Rosewood Scrub; Pine Mountain ; Redbank, 
 north of Laidley ; Tivoli; Kileoy Range. 
 
352 i 
 
 Thinnfeldia odontopteroides, var. faleata, Ten. Woods. 
 
 Loc. Rosewood, near Ipswich ; and Petrie’s Quarry, Brisbane. 
 Thinnfeldia media, Ten. Woods. 
 
 Zoe. Colinton. Occurs also at Burrum, 
 
 Family—PEcoPTERID®. 
 Genus—ALETHOPTERIS, Sternberg. 
 Alethopteris australis, Morris. 
 
 Loc. Bundanba New Chum ; Gray’s Seam, Ipswich; Rosewood, near Ipswich ; Kileoy Range; 
 Colinton; Six miles north of Esk; Peak Mountain; and Fassifern. Occurs also 
 at Burrum, and at Stewart’s Creek, Rockhampton. 
 
 Alethopteris Lindleyana (Royle), Feistmantel. 
 Loc. Redbank, near Mount Esk, north of Laidley. 
 
 Family—GLFIcHENIACER. 
 Genus—GLEICHENIA, Smith. 
 Gleichenia lineata, T. Woods. 
 Loe. Rosewood, near Ipswich. 
 
 Family—T2NIOPTERID&. 
 Genus—TNIoPrTeRIs, Brongniart. 
 Teniopteris (? Angiopteridium) Daintreei, McCoy. 
 Loc. Talgai; Rosewood, near Ipswich; Peak Mountain. Occurs also at Stewart’s Creek, 
 Rockhampton. 
 Teniopteris (2 Angiopteridium) Carruthersi, T. Woods. 
 Loc. Redbank, North of Laidley. Also at Stewart’s Creek, Rockhampton ?. 
 
 Genus—ANGIOPTERIDIUM, Schimper. 
 Angiopteridium, sp. ind. 
 Loc. Rosewood, near Ipswich. 
 
 Genus—Macrormnioprerts, Schimper. 
 Macroteniopteris wyanamatte, Feistmantel. 
 Loc. Ipswich. 
 
 Genus—SAGENoprerts, Presl. 
 Sagenopteris rhoifolia (Presl), Feistmantel. 
 Loc. Talgai, Darling Downs. 
 Sagenopteris cuneata, Carr., sp. 
 Loc. Tivoli Coal Mine, Ipswich. 
 
 Family—Dtioryorrerip™. 
 Genus—PHuerBorreris, Brongniart. 
 Phlebopteris alethopteroides, Eth. fil. 
 Loe. Darling Downs, near Toowoomba. 
 
 Section —PHANEROGAMIA. 
 Class—DIcoryLEDONES. 
 Order—CYcADACcE®. 
 Family—Zamirm. 
 Genus—PopozamiTzgs, F. Braun. 
 
 Podozamites lance:latus, Lindley and Hutton. 
 Loc. Ipswich Basin. 
 
 Podozamites sp. (Pl. 18, f. 5). 
 
 Loc. Redbank, north of Laidley. A somewhat similar plant (Pl. 18, f. 4) occurs at Burrum. 
 
i 
 
 858 
 
 Genus—PTEROPHYLLUM, Brongniart. 
 Pterophyllum abnorme, Eth. fil. 
 Loe. Redbank, north of Laidley. 
 Pterophyllum, sp. ind. (Pl. 16, f. 3). 
 Loe. Colinton. 
 
 Genus—Orozamitts, F. Braun. 
 Otozamites Mandeslohi, Kuryr. 
 Loe. Talgai. 
 
 Order—ConiIFERR. 
 Family—Taxacez. 
 Genus—Taxites, Brongniart. 
 Taxites medius, Ten. Woods. 
 Loe. Ipswich. 
 
 Genus—CUNNINGHAMITES, Sternberg. 
 Cunninghamites australis, Ten. Woods. 
 Loe. Rosewood, near Ipswich. 
 
 Genus—BRACHYPHYLLUM, Brongniart. 
 Brachyphyllum crassum, Ten. Woods. 
 Loc. Tivoli; Rosewood, near Ipswich ; Clifton. 
 
 Prants INCERTH SEDIS. 
 Genus—CARDIOCARPUM, Brongniart. 
 Cardiocarpum australe, Carruthers. 
 Loc. Tivoli. 
 
 Kingdom—ANIMALIA. 
 Sub-Kingdom—ARTHROPODA. 
 Class — CRUSTACEA. 
 Order—PHYLLOPODA. 
 Family—LIMNaDIDzZ, 
 Genus—HsTHERIA. 
 
 Estheria mangalensis, Jones. 
 
 Loc. Denmark Hill, Ipswich. 
 
 Class—InsEcra. 
 Order—COLEOPTERA. 
 Family—BUPRESTIDA. 
 Genus—MesostiaMoprERA, Etheridge fil. and Olliff. 
 Mesostigmodera typica, E. and O. 
 Loe. Denmark Hill, Ipswich. 
 
 Sub-Kingdom—Mo.uvsoa. 
 Section—MOoLLUSCA VERA. 
 Class—PELECYPODA. 
 Order—UNIONACER. 
 Family— UNIONID™. 
 Genus— Unto, Philipsson. 
 Unio ipsviciensis, Eth. fil., Pl. 42, figs, 2 and 3. 
 Loc. Bremer Basin Colliery. 
 Unio eyrensis, Tate? | 
 Loc. Bundanba. 
 ye 
 
354 
 
 SYNOPSIS. 
 
 and 
 
 Burrum Beds. 
 
 Occurring in Ipswich Beds. 
 
 Also in Burrum 
 Beds. 
 
 Also in Stewart's 
 
 Creek Beds 
 Also in Stewart’s 
 Creek Beds 
 
 
 
 x Hquisetum rotiferum, Ten. Woods. 
 ; ? latum, Ten. Woods. 
 Phyllotheca carnosa, 'Ten. Woods. 
 sp. ind. 
 Vertebraria equiset?, Ten. Woods. 
 Sphenopteris Baileyana, Ten. Woods. 
 x Trichomanites laxum, Ten. Woods ? 
 a spinifolia, Ten. Woods. 
 elongata, Carr. 
 Thinnfeldia odontopteroides, Morris. 
 rs var. falcata, Ten. Woods. 
 x 3 media, Ten. Woods. 
 x Alethopteris australis, Morris. 
 - Lindleyana (Royle), Feist. © 
 Gleichenia lineata, Ten. Woods 
 x Teniopteris (? Angiopteridium) Daintreei, McCoy. 
 x *: 2 Carruthersi, Ten. Woods. 
 Angiopteridum, sp. ind. 
 Phyllopteris Feistmanteli, Eth. fil. 
 Macroteniopteris wyanamatta, Feist. 
 Sagenopteris rhoifolia (Presl.) Feist. 
 Sagenopteris ? cuneata, Carr., sp. 
 Phlebopteris alethopteroides, Eth. fil. 
 Podozamites lanceolatus, L. and H. 
 sp. ind. (PL. 18, f. 5). 
 Pter ophyllum abnorme, Eth. fil. 
 = sp. ind. (PL. 16; £23): 
 Otozamites Mandeslohi, Kurr. 
 Taxites medius, Ten. Woods. 
 Cunninghamites australis, Ten. Woods. 
 Brachyphyllum crassum, Ten. Woods. 
 Cardiocarpum? australe, Carr. 
 Estheria mangalensis, Jones. 
 Mesostigmodera typica, Eth. fil. 
 Unio ipsviciensis, Eth. fil. 
 5 eyrensis, Tate. 
 
 
 
 
 
 
 
 
 
 
 
 Of the thirty-five species above named, three are common to the Stewart’s Creek (Rockhampton) 
 Beds ; two to the Burrum Beds; and two to both the Stewart’s Creek and Burrum Beds. 
 
 J. 
 
CHAPTER XXVIII. 
 
 THE TRIAS-JURA SYSTEM—continued. 
 
 THE IPSWICH FORMATION (UPPER TRIAS-JURA), OUTSIDE OF THE TYPE 
 DISTRICT. 
 
 IncLupiIn@ Stewart’s Creek (ROCKHAMPTON), AND Ros—Ewoop AND WYCARBAH (ROCKHAMPTON) 
 BrEps. 
 
 A very remarkable deposit occurs between the Central Railway at Stanwell and 
 Mount Lyon. A vast series of bedded basaltic rocks is here met with, having a slight 
 general dip to the north. Between, and beneath the beds of basalt, dark carbonaceous 
 shales, thin seams of impure coal, and beds of sandstone occasionally crop out. One bed of 
 ferruginous sandstone, near Mr. Lawrence’s Homestead on Stewart's Creek,* to which I 
 was guided by Captain Christoe in 1885, is full of well-preserved plant-remains. 
 
 At Wycarbah Railway Station, twenty-four miles from Rockhampton, a hard fine- 
 grained volcanic tuff is associated with the basaltic rocks. This tuff contains numerous 
 fern-impressions. The late Rev. J. E. Tenison Woods referred to the fossils of this 
 deposit + ‘‘as being of great interest, showing a relation with certain Mesozoic plant-beds 
 of India, which have never hitherto been identified outside that country.” 
 
 In his “ Fossil Flora’ the same Author referred (pp. 20, 45, 113, and 125) to plant- 
 
 beds at Rosewood, West of Rockhampton,{ containing Pétilophyllum oligoneurum, Ten. 
 Woods, Vertcbraria towarrensis, Ten. Woods, Sequoiites (?) australis, Ten. Woods, 
 Pecopteris, and Equisetum. 
 . In my “Handbook of Queensland Geology” (1885), I fell into 4 mistake in 
 understanding Mr. Tenison Woods to refer, in his Report to the Minister for Lands, 
 certain stratified deposits met with in the first twenty miles of the railway west of 
 Rockhampton (or more correctly from six to twenty miles), “containing marine shells 
 of well-known species found in the Lower Carboniferous rocks of Europe,’ to the same 
 deposit as the Stewart’s Creek (Rockhampton) Beds. In the same “ Handbook” I quoted 
 Glossopteris as occurring in the Stewart’s Creek Beds ; but the fossil in question, having 
 since been submitted to my Colleague, was pronounced to be not Glossopteris, but a 
 species of Phyllopteris. 
 
 Considerable collections of plants have, since 1885, been made by the late Mr. 
 James Smith and myself from the Stewart’s Creek, Rosewood, and Wyearbah beds. 
 There seems to be no reason why all the Mesozoic deposits within this limited district 
 should not be massed together and treated as a whole; and, in consideration of the 
 great similarity of their organic remains, I refer them to the Ipswich Jormation, 
 although I was at one time strongly inclined to regard the Stewart’s Creek, &c. (Rock- 
 hampton) Beds, as occupying a lower horizon than the Ipswich Beds, and as, in fact, 
 bridging over at least a part of the gap between the latter and the Burrum Coal 
 Measures. 
 
 * Not to be confounded with Stewart’s Creek, Townsville, where Permo-Carboniferous rocks occur. 
 
 + In a Report to the Minister for Lands, dated 7th August, 1883, published in the Queenslander News- 
 paper. 
 
 + Not to be confounded with Rosewood, near Ipswich, 
 
356 
 
 The following is a List of the Flora of the Stewart’s Creek (Rockhampton) Beds, 
 as determined or accepted by my Colleague :— 
 
 Kingdom—PLrantH. 
 Section—CRrYPTOGAMIA. 
 Class— ACOTYLEDONES. 
 Order—CaAtLaMARIE®, 
 Family—EQuviIsETace®. 
 Genus—EHquisetum, Linneus. 
 Equisetum rotiferum, Ten. Woods. 
 Loe. Stewart's Creek, Rosuhanpeo Occurs also in the Ipswich Coal Field. 
 Equisetum ? latum, Ten. Woods. 
 Loc. Rosewood, near Rockhampton. 
 
 Family—CaALaMITER. 
 Genus—VERTEBRARIA (Royle), McCoy. 
 Vertcbraria towarrensis, Ten. Woods. 
 Loe. Rosewood, near Rockhampton. 
 
 Family—PECOPTERIDE. 
 
 Genus—ALETHOPTERIS, Sternberg. 
 Alethopteris australis, Morris. : 
 | Loc. Stewart’s Creek, near Rockhampton. Occurs also in the Ipswich Coal Field and 
 Burrum Coal Field. 
 
 Family—T2NIopreRIDz&. 
 Genus—T2#NIOPTERIS, Brongniart. 
 Teniopteris (? Angiopteridium) Carruthersi, Ten. Woods. 
 Teniopteris (? Angiopteridium) Daintreet, McCoy. 
 Loc. Stewart's Creek, Rockhampton. Occurs also in the Ipswich Formation. 
 
 Genus—PHYLLOPTERIS, Saporta. 
 Phyllopteris Feistmanteli, Eth. fil. 
 Loc. Stewart’s Creek, Rockhampton. Occurs also in the Styx Coal Field. 
 
 Genus—M AcrorzNIoprTeRis, Schimper. 
 Macroteniopteris crassinervis, Feistmantel. ? 
 Loc. Wycarbah, near Rockhampton. 
 
 Section—PHANEROGAMIA. 
 Class—DIcoTyLEDONES. 
 Order—CYoaDACEz. 
 Family—ZAMInR. 
 Genus—PTILoPHYLLuM, Morris. 
 Ptilophyllum oligoneurwm, Ten. Woods. 
 Loc. Rosewood and Wycarbah, near Rockhampton. 
 
 Order—ConIFERz. 
 Family—ARAUCARIE. 
 Genus—ARAUCARITES, Sternberg. 
 Araucarites ? polycarpa, Ten. Woods. 
 Loe. Stewart’s Creek, Rockhampton. 
 
 Family—TAaxopiacem. 
 Genus—Srquoiites, Carruthers. 
 Sequoiites ? australis, Ten. Woods. 
 Loe. Rosewood, near Rockhampton. 
 
 PoantH InceRtTm SuEDIs. 
 Genus—Crcapinocarets, Schimper. 
 Cycadinocarpus ? sp. ind. 
 Loe. Wycarbah. 
 
357 
 
 Quite recently a discovery of coal, which must assume considerable importance 
 when railway communication has been established, was accidentally made by a party of 
 prospectors subsidised by the Government (Messrs. Petersen, Otty, and Dunn), when 
 sinking a shaft in search of alluvial gold. The locality is about fifty-two miles south- 
 west of Gladstone, and about three miles north-west of the Old Callide Station, on 
 Callide Creek. A Report * by Mr. W. H. Rands, just issued, enables me to give an 
 account of this Coalfield. 
 
 The lowest beds of the Coal Measures rest unconformably on Paleozoic rocks, 
 which Mr. Rands says may be Permo-Carboniferous (? Gympie Series). They consist 
 of conglomerates, sandstones, and shales, forming an escarpment of two hundred feet 
 in height, and dip at 19° to 8S. 27° W. These strata are overlaid by a bed of close- 
 grained olivine-basalt, which dips in the same direction, but at a lower angle. The 
 stratified rocks re-emerge from beneath this lava-flow, at a lower elevation, further to 
 the west, but are covered on the higher ridges with patches of basalt. Regarding the 
 age of the coal-bearing strata, Mr. Rands says :— 
 
 “T found two varieties of plant-remains in athin bed of indurated clay in the 
 gully near Shaft No. 3. One of these closely resembles the description given by Pro- 
 fessor Ottokar Feistmantel} of Thinnfeldia odontopteroides, Morris, except that the 
 pinnules appear to be divided at the base, instead of being “connate.’’ This fossil is 
 found in both the Hawkesbury and in the Wianamatta Series, New South Wales; and 
 in the Upper Mesozoic Beds of Ipswich. This form is very numerous here. The other 
 isa species of Teniopteris, in which the veins are parallel, and about one-thirteenth of an 
 inch apart. These remains would point to the beds belonging to the Upper Mesozoic, 
 and probably they are the same age as the Ipswich Beds.” 
 
 The following remarks are taken from Mr. Rands’ description of the coal-seams : — 
 
 “ Shaft No. 1.—The top eight feet is timbered, but I understand that it consisted 
 efa black carbonaceous shale or clod. 
 
 Tt. in. 
 Timbered 8 0 
 Coal (with a l-inch Hand of clay at 65 feet from. tite tp, ae ag Linch 
 
 band at 7 feet from the top ... . = 10.5 
 
 Greyish brown sandstone, thinning out “£6 a mere Usteeake on one 
 side of the shaft.. 
 
 Coal (three feet of he were ander acta a Fis nt oye AY 
 Hard carbonaceous sandstone ; thickness unknown. 
 
 “The top ten feet of coal is of asomewhat friable character, but the bottom seven 
 feet is a good strong coal. Analyses of this coal are given below, and from the analyses and 
 appearance it should make a good steam coal. The beds just here are nearly horizontal. 
 
 “ Shaft No. 2.—The shaft was partially filled with water, so that I was unable to 
 descend. They are reported to have passed through in sinking— 
 
 Ft. in. 
 Greyish sandstone ... ot Pe a te eee our) 
 Black carbonaceous shale or ralode a oes vt nes Rete 
 Coal, not bottomed . ae ai ; ay oa we hd Gime U 
 
 “The large heap of pal on the sur ee is a bright, lean coal. Ananalysis of the 
 coal is given below. The coal from this shaft appeared to consist toa great extent 
 of Sporangia. Icuta thin section for the microscope, and found it to be full of small 
 circular spores, which appear brown in the almost opaque coal. I believe these to be 
 Sporangia, but I found great difficulty in getting the section fully transparent. 
 
 
 
 * New Discovery of Coal near the Callide Creek, Port Curtis District. Brisbane : by Authority : 1891, 
 
 + Geol. Pal. Relations Coal and Plant-bearing Beds of E. Australia, JZem, Gol. Survey N.S. Wales, 
 Pal, No. 3, p. 101. 
 
358 
 
 ‘“ No. 3 Shaft.—There were four feet of water in the bottom of the shaft, but I 
 was able to descend and examine it down to that depth. The shaft passed through— 
 
 Ft. in. 
 Grey sandstone ey aie gt nb see oe 
 Brown shales and clay ve - et a sor i 30 O 
 Black carbonaceous shale or clod mt re 
 Coal (twenty-six feet of this was above the water) ie we peer lth at. 
 
 “T could discover no bands in the twenty-six feet of coal visible. Itis aclean coal. 
 The beds dip slightly north-east. 
 
 “ Shaft No. 6 is forty feet, but it was nearly full of water. I was informed by 
 the prospectors that the coal in this shaft was twenty-four feet thick, with a thin band at 
 about eleven feet from the top of the seam. The following section was given to me as 
 
 approximately correct :— Ft. in. 
 Sandstone and black carbonaceous shale sil ar ee ct Loma 
 Coder... AS at fe ni a a $4: aX, Cee Lee 
 Codi we , : son ips 
 
 “ No coal has hearea seen quinine cropping pul e the Airfare: 
 “The following are Approximate Analyses of the coals made for me by Mr. W. A. 
 Dixons ce F.CS., of the Technical College, Sydney :— 
 
 | SHAFT No. 1. 
 
 
 
 i] 
 aaa Shaft No. 2. Shaft No. 3. 
 Top portion of the | Bottom portion of 
 | seam. the seam. 
 
 Moisture ¥ a oo 8:35 8:40 9°15 9 95 
 Volatile hydr ocarbons nt sot 28°79 24°49 26°71 23°63 
 Fixed carbon ... se ~ ey | 41°74, 57°36 5124 54:20 
 Asi aes. mn en Se me 20°78 9°50 12°62 12°04. 
 Sulphur | 0°34 0:25 0:28 0:18 
 
 
 
 
 
 | 100:00 100:00 100°00 100°00 
 
 
 
 
 
 “Mr. Dixon adds: ‘ None of the samples yield any truecoke. The ashis in each of 
 them perfectly white and rather gritty. Thesamplefrom Shaft No. 1, top portion of the 
 seam, is rather tender, whilst the others are strong, and have the appearance of splint 
 coal, but the analysis shows that they belong rather to the class of lignite than true coal.’ 
 
 “The following Analysis was made by Mr. J. Cosmo Newbery, for Mr. Spiers, of 
 Rockhampton. The sample was from Shaft No. 1, but I do not know which portion of 
 the seam it is from. The analysis is, like that of Mr. Dixon’s, from the bottom portion 
 of the seam, but it contains less ash :— 
 
 
 
 Moisture at ae ne wre ae ae AD LO 
 Volatile hydrocarbons 3 cee Sec ee ... 26365 
 Fixed carbon ... ee ee 58 rie Be ... 99°850 
 Ash a ata = aa ann Ree rare sore AGS 
 
 100°000 
 
 “The coal is non-coking, and gives a light white ash. 
 
 “The analysis would point to the coal being a good steam coal, though the 
 calorimetric power of tbe coal requires testing. 
 
 ‘“‘ The sample from the top portion of the seam from Shaft No. 1 gave so high a per- 
 centage of ash that I determined to try another sample, with the result that I obtained 
 46 as a percentage of ash. Itis very probable, therefore, that the sample sent to Mr. 
 Dixon for analysis had asmall impure coaly band in it.” ; 
 
CHAPTER XXIX. 
 
 THE TRIAS-JURA SYSTEM—continued. 
 
 THE IPSWICH FORMATION (UPPER TRIAS-JURA); ITS AGE AND RELATIONS. 
 
 Tw his Paper “On the Geology of Queensland,” read in 1872 before the Geological Society 
 of London,* the late Mr. Richard Daintree insisted on the importance of the two ferns 
 Glossopteris and Teniopteris as characteristic, the former of the Palmozoic, and the 
 latter of the Mesozoic Coal Deposits. The late Rev. Julian E. Tenison Woods, in his 
 “Fossil Flora of the Coal Deposits of Australia’’ (p.11), remarked that “ the selection of 
 Teniopteris is unfortunate, because it is not common,t and probably included distinet 
 genera, according to the classification then adopted. Thinnfeldia is a much better 
 typical fossil of the Mesozoic Beds, and it is never found associated with Glossopteris. It 
 is very common and prevails everywhere in Oolitic plant-beds.”{ On the ground that 
 TLeniopteris was common to them all, Mr. Daintree regarded the Ipswich Coal Forma- 
 tion as the equivalent of “the Txniopteris Coal Measures of Victoria and of the 
 Richmond River, N.S.W.”’ To Daintree Mr. Tenison Woods (Joc. cit.) assigns ‘the 
 eredit of co-relating the Jerusalem (Tasmanian) Beds with those of Ipswich,” but I 
 cannot find any warrant for this in Daintree’s Paper itself. 
 
 Mr. Tenison Woods, at one time,§ classed the Ipswich Coal Measures as 
 Jurassic, and placed the Desert Sandstone on the same horizon. This view as to the 
 position of the Desert Sandstone never was entertained by any other Geologist, 
 and is obviously incorrect, when it is considered that that formation actually overlies 
 unconformably the Rolling Downs Formation, which is itself newer than the Ipswich 
 Formation. It was abandoned by Mr. Tenison Woods himself in his latest account of 
 the Desert Sandstone || in favour of an idea not less untenable—viz., that “it [the 
 Desert Sandstone] probably belongs to the two great volcanic periods of Tertiary age.” 
 
 Mr. Woods further placed on the same horizon as the Ipswich Beds the Clarence 
 River Beds, and the Hawkesbury Sandstone of New South Wales. The Ipswich Beds 
 cross the border into New South Wales, where they are known as the “‘ Clarence Series.” 
 The latter contains, according to the late Mr Charles 8. Wilkinson, Government Geologist 
 of New South Wales, no Glossopteris, but Teniopteris Daintreei, Alethopteris 
 australis, and Thinnfeldia, and may be newer than the Wianamatta Beds, and of the 
 same age (Jurassic) as the Victorian Coal Series of which Teinopteris Daintreet is 
 a characteristic fossil.{_ Mr. Wilkinson’s observations ** may be quoted to show the 
 distinction between the Hawkesbury and Wianamatta Beds. 
 
 “The surface of the Hawkesbury formation was denuded and worn into hollows 
 before the Wianamatta beds were deposited; and the latter in their lithological 
 
 * Quart. Journ. Geol. Soc., 1872, Vol. xxviii., p. 288. 
 
 + Several sections of Zeniopteris are very common indeed in many localities within the ‘‘ Ipswich” 
 and Stewart’s Creek (Rockhampton) areas. (R.Z. Junr.) 
 
 t The value of Zeniopteris, using the genus in the widest acceptance of the term, as marking the 
 presence of Mesozoic Beds as against those of Permo-Carboniferous age, holds now as good as when 
 Mr. Daintree wrote. In Queensland Zeniopteris has not yet been found lower than the Burrum (Styx) 
 Coal Measures. (2.2L. Junr.) 
 
 § Flora, pp. 18 and 19. 
 
 || Journ, R. Soc. N. S. Wales, 1888, xxii., p. 290. 
 
 {| Notes on the Geology of New South Wales, 1882, p, 55, 
 
 BLOCH City De Oks 
 
360 
 
 cha acter also show that great physical changes must have taken place, for they con- 
 sist chiefly of argillaceous shales, which are in striking contrast with the thick-bedded 
 arenaceous rocks underlying them. The fine sediment which formed the Wiannamatta 
 shales evidently settled down in the quiet waters of a lake.” 
 
 Both the Hawkesbury and the Wianamatta Beds contain plants which are 
 common in the Ipswich Formation and in the Clarence Beds,and both contain, in addition, 
 remarkable deposits of fish remains,* of which the Ipswich and Clarence Beds have, so 
 far as | am aware, as yet furnished no equivalent. 
 
 As for the last two years the Stratigraphy and Paleontology of the Mesozoic rocks 
 of New South Wales have been closely studied by the late Mr. C. 8. Wilkinson, Mr. 
 (now Professor) T. W. Edgeworth David, and my Colleague, we are enabled to give the 
 latest views of the Geological Survey in the following concise table + :— 
 
 eae 
 Teniopteris beds of Talbragar River, and part of the Clarence District. 
 
 70). Wianamatta Shales, with Macroteniopteris, Thinnfeldia, &c. 
 
 1,000. Hawkesbury Sandstone, with Thinnfeldia, Palconiscus, Platiceps 
 
 Triassic Wilkinsoni, &e. 
 P Ballimore Beds. , 
 800. Narrabeen Shales, with Thinnfeldia, and Estheria and intercalated 
 cupriferous tufts. 
 
 In Victoria, Mr. Reginald A. F. Murray, following Mr. Wilkinson, accepts f 
 the Carbonaceous (? Oolitic) rocks of the Wannon, Cape Otway, Western Port, and 
 South Gippsland as the equivalent of the Clarence River Beds, and the Bacchus Marsh 
 Sandstones as the equivalent of the Hawkesbury Sandstones, there being no recognised 
 equivalent of the Wianamatta Beds. The “ Carbonaceous (? Oolitic) rocks” contain 
 Zamites (Podozamites) Barklyi, McCoy; Zamites (Podozamites) ellipticus, McCoy ; 
 Zamites longifolius, McCoy; Teniopteris Daintreei, McCoy; and Alethopteris (Pecopteris) 
 australis, Morris, whose nearest European ally is Pecopteris scarburgensis, Bean, MS. 
 as determined by Prof. Sir F. MeCoy.§ 
 
 In Tasmania “ the rocks of Mesozoic age consist mainly of variegated sandstones, 
 shales, blue and white clays, often of great thickness, and extending throughout the 
 midland, southern, and south-eastern districts. They frequently contain seams of coal, 
 sometimes, as in the Fingal District, of great thickness and of fair quality. The beds 
 of the system are distributed in distinct basins, often greatly disturbed and broken up 
 by intrusive dykes of greenstone, and on this account, and because of the great sameness 
 of plant-remains, there is great difficulty in attempting to break up the beds 
 of the system into subdivisions. The beds probably cover the whole period from 
 the close of the Upper Paleozoie Coal Measures to the beginning of the Tertiary 
 Period. No marine deposits break the sequence, as in Queensland. The great Lignite 
 and Leaf Bed Series (Paleogene) with leaves of oaks, elms, laurels, beech, cinnamon, 
 and other trees, generally overlie the Mesozoic members in the Launceston Tertiary 
 Basin.” 
 
 The “ Upper (Mesozoic) Coal Measures” are developed at Derwent, Jerusalem, 
 Fingal, Longford, Hamilton, Spring Bay, Port Cygnet Basins, &e. An “ Older Sand- 
 
 
 
 
 
 * See Memoirs of the Geological Survey of New South Wales, Pal., No. 4. ‘‘The Fossil Fishes of 
 the Hawkesbury Series at Gosford.” By Arthur Smith Woodward, F.Z.8.,F.G.S. Sydney: by Authority: 
 1890. 
 
 + A Correlation of the Coalfields of New South Wales. By T. W. E. David, B.A., F.G.S. Proc. 
 Austr. Assoc. Adv. Scz., Vol. ii., 1890, p. 464. 
 
 + Geology and Physical Geography of Victoria. Melbourne: by Authority: 1887. 
 
 § Prodromus of the Paleontology of Victoria, Decade i., 1874, and Decade ii., 1875. 
 
361 
 
 stone Formation,” consisting of “reddish or yellow micaceous sandstones, sometimes 
 of great thickness, often occurs overlying the uppermost beds of the Upper Paizozoie 
 mudstones, as at Tinder Box Bay, Huon Road, and Waterworks Valley, near Hobart, 
 with indistinet plant-impressions and silicified trunks of conifers. These sandstones 
 apparently lie conformably, and without stratigraphic break, upon the uppermost beds 
 of the Upper Marine series. Their position is assigned, provisionally, at the base of 
 the Mesozoic group of rocks of Tasmania.”’* 
 
 The majority of the plants characteristic of the Ipswich Formation are met with, 
 according to Mr. Johnston’s lists, in the Upper Coal Measures of Tasmania, and many 
 others besides. It must be pointed out that Mr. Johnston obtained from the same 
 locality (Lord’s Hill, Newtown) Glossopteris (G. moribunda, Johnston) and Teniopteris 
 (2. tasmanica, Johnston).t 
 
 If the Tasmanian Mesozoic Beds, as Mr. Johnston supposes, cover, without a 
 break, “the whole period from the close of the Upper Paleozoic coal measures to the 
 beginning of the Tertiary period,” the Ipswich Formation can only represent a small 
 portion of the same time, as between the Ipswich Beds and the Tertiary, the whole 
 period represented by the Rolling Downs and Desert Sandstone, and the uncon- 
 formability between them, must intervene—and that was certainly of no insignificant 
 duration. ; 
 
 In New Zealand “The most valuable coal deposits occur in the Cretaceo-tertiary 
 formation—but always beneath such of the marine beds of the formation as are present 
 in the locality where the coal occurs. The coal-bearing beds always rest upon the 
 basement rock of the district [slates and granites] marking a great unconformity and the 
 closing of a long-persistent land area at the period to which they belong.”’{ Itis evident 
 that this Coal Field can have nothing in common, so far as its age is concerned, with the 
 Ipswich Coal Field. 
 
 Older than the Cretaceo-Tertiary Coal Fields are the Buller Series, consisting 
 of conglomerate and sandstones, with coal-seams, and the Amuri Series, consisting of 
 green and grey incoherent sandstones, with hard concretions and large masses of 
 silicified wood. “This formation, which is confined to a few localities of limited extent, 
 is very rich in fossils of the genera Belemnites and Trigonia, with a few saurian bones 
 and teeth of large chimeroid fishes.Ӥ The Buller and Amuri Series are classed by the 
 Geological Survey of New Zealand as Lower Gi'eensand. 
 
 Next in order come the Mataura, Putataka, and Flag Hill Series, classed by the 
 Geological Survey as Jurassic. The Mataura series “ consists largely of estuarine beds, 
 marine fossils being absent or rare. It consists of dark-coloured marls and fine-grained 
 sandstones, and contains the fossil remains of a number of plants, of which eight species 
 have been recognised. Amongst these are Camptopteris, Oycadites, and Echinostrobus, 
 which connect them with the plant-beds of the next lower formation. Those found at 
 Waikawa and Mataura Falls are especially interesting, from at least one species, 
 Macroteniopteris lata, being identical with a plant found in the Rajmahal beds of India, 
 which are considered to be of Liassic age. . . . . The Mataura series, overlying the 
 Putataka series, closes the old secondary sequence at Kawhia, in the Auckland District, 
 and the same plants are found in the Clent Hills plant-beds, and from the natural sections, 
 
 
 
 * Systematic Account of the Geology of Tasmania, p. 149. By Robt. M. Johnston, F.L.S., &c. 
 Hobart: by Authority: 1888. 
 
 Ho Op: Cit. Ds Lit. 
 
 t Catalogue and Guide to the Geological Exhibits, New Zealand Court, Indian and Colonial Exhibition, 
 p. 59. By Sir James Hector, Director of the Geological Survey. Wellington : by Authority: 1886, 
 
 § Op. cit., p. 63. 
 
362 
 and also from the very characteristic forms below them, there can be no doubt that they 
 should be referred to the Upper Oolite period. . . . . The Putataka beds are of 
 marine origin, and contain Middle Oolite fossils.” The Flag Hill series is marine.* 
 
 It may be conjectured that the Mataura Beds represent at least some portion of 
 the Ipswich Formation, but the preponderance of marine beds in the Mesozoic Trias of 
 New Zealand presents a striking contrast to Tasmania. 
 
 Of the whole Queensland Mesozoic System, between the uppermost fresh-water 
 Coal Measures of the Bowen River Coal Field (Permo-Carboniferous), and the Rolling 
 ~ Downs Formation (Cretaceous), z.e., the Burrum, Stewart’s Creek (Rockhampton), and 
 Ipswich Beds, my Colleague says that the organic remains are principally those of 
 plants, with a strong Mesozoic facies, and oscillating in all probability between the Trias 
 and Upper Oolite in age. Since he expressed the above opinion, however, my 
 Colleague has, together with Professor Edgeworth David, attributed a Triassic age to 
 some of the New South Wales equivalents of the Ipswich (and Burrum?) Formations. 
 As the Mesozoic Formations have been more closely studied in New South Wales, it 
 will be well to extend the range of the Queensland (Burrum and Ipswich) downward 
 to the base of the Trias. As, on the other hand, the Ipswich Formation appears to 
 graduate upwards, without break, into the Cretaceous of the Rolling Downs, it is 
 probable that the Queensland strata cover the whole of the time between the base of 
 the Trias and the top of the Oolite. It thus becomes convenient to classify the 
 Burrum and Ipswich Formations respectively as Lower and Upper Trias-Jura. 
 
 It is possible that in the sandstones of Murphy’s Creek and other localities on 
 the slopes of the Toowoomba Range, we may have the equivalents of the Hawkesbury 
 Sandstones. 
 
 The following is my Colleague’s List of the Fossils from the whole of the 
 Queensland strata which are grouped together under the name of the Ipswich 
 Formation :— 
 
 Kingdom—PLanTm. Family —NEUROPTERID 2. 
 Section—CRYPTOGAMIA. * Genus—THINNFELDIA. 
 Class—ACOTYLEDONES. Thinnfeldia odontopteroides, Morris. 
 Order—CALAMARIE®. _ 3 var. falcata, Ten. 
 Family—EqQuisEracen. Woods. 
 
 Genus—EQuisETUM. » media, Ten. Woods. 
 
 Equisetum rotiferum, Ten. Woods. 
 »  ¢latum, Ten. Woods. 
 Family—ScuHizONEURES. 
 Genus—PHYLLOTHECA. 
 Phyllotheca carnosa, Ten. Woods. 
 
 Family—PErcoPprEeRIDm. 
 Genus—ALETHOPTERIS. 
 Alethopteris australis, Morris. 
 rf Lindleyana, Feist. 
 
 " ‘sp. ind., Pl. 42, fig. 1. Family—GLEICHENIACER. 
 Family--CaLaMire x. Genus—GLEICHENIA. 
 Genus—VERTEBRARIA. Gleichenia lineata, Ten. Woods. 
 
 Vertebraria equiseti, Ten. Woods. Family—T-msr1oprerrp™. 
 
 i towarrensis, Ten. Woods. ity ieee cone nem 
 Order—FI1iczs. Teniopteris (? Angiopteridium) Daintreei, Ten. 
 Family —SPHENOPTERID®. el sete! 
 
 Genus—SPHENOPTERIS. Teniopteris (? Angiopteridium), Carr. 
 
 Sphenopteris Baileyana, Ten. Woods. 
 Genus—ANGIOPTERIDIUM. 
 
 Genus—TRICHOMANITES, : ps : 
 Angiopteridium, sp. ind. 
 
 Trichomanites lacum, Ten. Woods. ? 
 - spinifolia, Ten. Woods. Genus—PHYLLOPTERIS. 
 - elongata, Carr. Phyllopteris Feistmanteli, Eth. fil. 
 
 
 
 
 
 * Op. cit., pp. 65-68, 
 
363 
 
 Genus—MAcROTENIOPTERIS. 
 Macroteniopteris wianamatta, Feist. 
 ie crassinervis, Feist. 
 
 7 sp. ind. 
 
 Genus—SsGENOPTERIS. 
 Sagenopteris rhoifolia, Presl. 
 oe ? cuneata, Carr. | 
 
 Family—D10ryoPreRiIpDz&. 
 Genus —PHLEBOPTERIS. 
 Phlebopteris alethopteroides, Eth. fil. 
 
 Section—PHANEROGAMIA. 
 Class—DICoTYLEDONES. 
 Order—CYCADACER, 
 Family—ZamMiem. 
 Genus—PopoZAMITEs. 
 Podozamites lanceolatus, Lindley and Hutton. ? 
 * sp. ind. 
 
 Genus—OTOZAMITES. 
 Otozamites Mandeslohi, Kurr, 
 
 Genus—PTEROPHYLLUM. 
 Pterophyllum abnorme, Eth. fil. 
 8 sp. ind., Pl. 16, fig. 3. 
 
 Genus—PrILoPHYLLUM. 
 Ptilophyllum oligoneurum, Ten. Woods. 
 
 Order—ContFEeR&. 
 
 Family—ARAUCARIZ®. 
 
 Genus— ARAUCARITES. 
 Areucarites ? polycarpa, Ten. Woods. 
 
 Family—Taxopiacem. 
 Genus—SEQUOITES. 
 Sequoites ? australis, Ten. Woods. 
 
 Family—TAxacre®. 
 Genus—TAXITES. 
 Taxites medius, Ten. Woods. 
 
 Genus —BRACHYPHYLLUM. 
 Brachyphyllum crassum, Ten. Woods. 
 
 Genus—CUNNINGHAMITES. 
 Cunninghamites australis, Ten. Woods. 
 
 Prant& INcERT#® SsEDIS. 
 Genus—CARDIOCARPUM. 
 Cardiocarpum ? australe, Carr. 
 
 Kingdom—ANIMALIA. 
 Sub-Kingdom—ARTHROPODA. 
 Class—CRUSTACEA. 
 Order—PHYLLOPODA. 
 Family—LImMNnaDIp&. 
 Genus—EHstTHERIA. 
 
 Estheria mangaliensis, Jones. 
 
 
 
 Class—INSECTA. 
 
 Order—CoLEoPtERA. 
 
 Genus—MeEsosTIGMODERA. 
 Mesostigmodera typica, Eth. fil. and Ollff. 
 
 
 
 Sub-Kingdom—Mo.uusca. 
 Section—MoLLUSCA VERA. 
 Class—PELECYPODA, 
 Order— UNIONACE. 
 Family—UNIONIDE. 
 Genus—UNI0. 
 
 Unio ipsviciensis, Eth. fil. 
 
 Unio eyrensis, Tate. 
 
 In the above list we have five species of plants—viz.: Trichomanides laxum, 
 Thinnfeldia media, Teniopteris Daintreet, Phyllopteris Feistmanteli, and Alethopteris 
 australis, common to the Burrum beds. 
 
 Although, so far as we know, there is no evidence of a break between the 
 Ipswich and Rolling Downs Formation, but, on the contrary, everything points to an 
 uninterrupted succession, the whole of the above copious flora is unrepresented in the 
 Rolling Downs Formation. This circumstance, however, may mean nothing more than a 
 change from terrestrial or lacustrine to marine conditions. Two species (but not the 
 same) of Unio occur both in the Ipswich and Rolling Downs Formations. 
 
 Again, in spite of the moderately large list of plants and marine organisms 
 furnished by the Desert Sandstone (Upper Cretaceous), the latter has not a single 
 species, or even genus, in common with the Ipswich Formation. 
 
 J. 
 
CHAPTER XXX. 
 
 THE ORGANIC REMAINS OF THE IPSWICH FORMATION 
 (UPPER TRIAS-JURA), 
 
 Wirn Descriprions OF THE SPECIES. 
 Kingdom—PLANTA. 
 Section—CRYPTOGAMIA. 
 CLAss—ACOTYLEDONES. 
 
 Order—CALAMARIEE. 
 Family—EQUISETACE. 
 
 
 
 Genus—EQUISETUM, Linneus, 1778. 
 
 (Gen. Plantarum, 554.) 
 EQUISETUM ROTIFERUM, Zen. Woods. 
 
 Equisetum rotiferum, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1882, vii., Pt. 3, p. 344. 
 x ¥ Ten. Woods, loc. cit., 1883, viii., Pt. 1, p, 66, t. 6, f. 5 and 6. 
 
 Sp. Char. ‘Stem cylindrical, closely and faintly grooved, joints approximate 
 below, distant above, ieaves carinate, conate into a sheath, the teeth of which are short, 
 flat, round, of equal width throughout, adpressed to the stem. The diaphragmata of 
 the joints and leaf-scars of the branches are very distinct, round, with radiate lamine 
 varying from eighteen to thirty, and a central orifice. Fructification unknown.” 
 
 Obs. The general appearance of the fragmentary remains of this plant is thus 
 given by the Rev. J. HE. T. Woods. ‘There are certain disk-like forms of rather an 
 ornamental character. They are shaped like toothed wheels, with a small central 
 perforation, and a radiate ring of pear-shaped perforations near the edge.” The present 
 plant appears to be related to Hquisetum rajmahalensis,* the diaphragm in the two 
 species being similar. 
 
 In Pl. 16, fig. 9, a phragma of an equisetaceous plant is figured. Although twice 
 the natural size, it will be seen that this is far larger than the specimen figured by the 
 Rev. J. E. T. Woods. Until we know more of the fragmentary remains of these 
 Mesozoic plants it would be rash to determine such a specimen. From the same locality 
 as the last plant referred to, a portion of a stem has been obtained. It is an internode 
 of rather more than one inch in length and about seven-sixteenths of an inch broad, and 
 the surface microscopically striate parallel to the longer axis. One of the ends is 
 terminated by a well-marked point of articulation. 
 
 Loc. Walloon Mine, Ipswich. Grey fireclays above first coal-seam (The late 
 Rev. J. E. T. Woods; Macleay Museum, University of Sydney). Stewart’s Creek, 
 near Rockhampton (The late James Smith). 
 
 * Mem. Geol. Survey of India; Paleontologia Indica; Fossil Flora of the Gondwana System. Oldham 
 and Feistmantel, Vol. i., Pl. 11, f. 3. 
 
365 
 
 EqQuiIsETUM ? LatuM, Ten. Woods. 
 Equisetum ? latum, Ten. Woods, Proc. Linn. Soc. N. &. Wales, 1883, viii., Pt. 1, p. 87, t. 2, f. 1. 
 
 Sp. Char. “ Broad stems two or three inches wide, with numerous small close 
 ribs.” 
 
 Obs. There are, according to the describer, about twenty ribs to an inch. It 
 is compared to Hquisetum Mougeotti, Brong., a Trias fossil of the Vosges. The Mining 
 and Geological Museum, Sydney, contains examples of an Hywisetum, believed to be 
 this species, eight inches in length and two and a half in width, and bearing about the 
 same number of delicate ribs to the inch as mentioned by Mr. Woods. The mean of a 
 number of computations is twenty-three. 
 
 Loc. Esk Valley, forty-six miles west-north-west of Ipswich (W. Souttar ; Mining 
 and Geol. Museum, Sydney); Rosewood, near Rockhampton (The late Rev. J. E. T. 
 Woods ; Macleay Museum, University of Sydney). 
 
 Family—SCHIZONEURE. 
 
 Genus—PHYLLOTHECA, Brongniart, 1828. 
 (Prod. Hist. Vég. Foss., p. 151.) 
 
 Obs. Phyllotheca has been described as a Queensland genus by the late Rey. 
 J. E. T. Woods, but his remarks are somewhat contradictory as to its occurrence. In the 
 early part (p. 18) of his Memoir “On the Fossil Flora of the Coal Deposits of Australia’ + 
 he quotes Phyllotheca concinna as found in the Ipswich Beds, but later (p. 39), when this 
 species is described, its range is confined to the Hawkesbury Sandstone of New South 
 Wales. 
 
 Again he says, “ For my own part, after a careful search, I have never found any 
 true or characteristic Phyllotheca in the Ipswich Coal Beds.” Then why describe the 
 following species immediately after, as he does, without a note of interrogation after 
 the genus. Phyllotheca was identified by the Rev. Author from the Cooktown Coal 
 Beds * (Permo-Carboniferous), but this was abandoned in his larger Memoir. 
 
 PHYLLOTHECA CARNOSA, Zen. Woods. 
 Phyllotheca carnosa, Ten, Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., Pt. 1, p. 75, t. 9, f. 2. 
 
 Obs. This species was named from a faint impression, imperfect, but showing 
 a “close succession of verticillate leaves, which radiate very slightly from the stem. 
 They are close, obtuse, about half a millimetre wide, and five long. They form five cup- 
 shaped divisions on a stem thirty-five millimetres long and ten wide.’’ It is considered 
 by Mr. Woods to be an ally of P. robusta of the Indian Lias. The specimens at present 
 in the Macleay Museum are quite unworthy of a name. 
 
 Loc. Walloon Mine, Ipswich (The late Rev. J. LE. T. Woods ; Macleay Museum, 
 University of Sydney). 
 
 PHYLLOTHECA, sp. ind., Pl. 42, fig. 1. 
 
 Obs. A few small whorls of lanceolate leaves have presented themselves from 
 Bundanba. There are fourteen in a circlet, the largest measuring eight millimetres, 
 and the opening left by the decay of the stem measuring two millimetres. The leaves 
 are short and lanceolate, and their bases appear to be sessile or decurrent, on the 
 
 * Proc. Linn. Soc. N. S. Wales, 1882, vii. p. 95. 
 ‘++ Author’s separate copy. 
 
366 
 
 internode. The arrangement is similar to McCoy’s figure of Phyllotheca ramosa,* but 
 there is even a greater resemblance to Feistmantel’s illustration of P. robusta t from the 
 Lower Gondwanas. 
 
 Loc. Borehole Colliery, Bundanba, near Ipswich (2. C. Ringrose). 
 
 Family—CALAMITEA. 
 
 Genus—VERTEBRARIA (Royle), McCoy, 1847. 
 (Ann. and Mag. Nat. Hist, 1847, xx., p. 145.) 
 
 VERTEBRARIA EQUISETI, Zen. Woods. 
 Vertebraria equiseti, Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. 1, p. 80, t. 1, f. 3. 
 
 Sp. Char. Roots found in broad, finely striated masses, three or four inches 
 long, with occasional transverse divisions half an inch or so across. (Ten. Woods.) 
 
 Obs. Mr. Woods states that three different kinds of roots can be distinguished. 
 
 ‘A broad striated stem, half an inch in diameter, with transverse divisions at 
 irregular intervals.” 
 
 “A narrow cylindrical stem with parallel striations, and no diaphragmata.”’ 
 
 “Stems with a central longitudinal division and irregular transverse diaphrag- 
 mata, which occasionally correspond at each side of the longitudinal line and occasionally 
 do not.” 
 
 These bodies are believed to be the rhizomes of Equisetum rotiferum. 
 
 Loc. The Author says, “I shall distinguish the Vertebraria common in the blue 
 clay at the Walloon Mines as V. equiseti.”” Further on he adds, “ Found in grey clay 
 below the coal in the Tivoli Mine.” The latter locality is confirmed by my Colleague. 
 
 VERTEBRARIA TOWARRENSIS, Ten. Woods. 
 Vertebraria Towarrensis, Ten. Woods, Proc. Linn, Soc. N.S. Wales, 1883, viii., Pt. 1, p. 81, t. 1, f. 1, 2, 
 and 4. ; 
 
 Sp. Char. Broad stems with deep or regular longitudinal grooves, but with 
 slight transverse divisions, which are irregular, at long distances apart, or absent. 
 (Len. Woods.) ; 
 
 Obs. The parallel lines are described as regular in some specimens, in others 
 they curve, twist, and fold over one another. There is a general resemblance between 
 these fossils and Vertebraria, but they are very dubious-looking plant-remains. 
 
 Loe. . Rosewood, twenty four miles west of Rockhampton (The late Rev. J. L. T. 
 Woods; Macleay Museum, University of Sydney). 
 
 Order—FILICES. 
 Family—SPHENOPTERID. 
 
 Genus—SPHENOPTERIS, Brongniart, 1828. 
 (Prod. Hist. Vég. Foss., p. 50.) 
 SPHENOPTERIS BatLEyana, Ten. Woods. 
 
 Sphenopteris (Hymenophyllum) Baileyana, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, Wills, beatles 
 ; D. 93; ta 4, fee 
 Sp. Char. Frond bi-pinnatifid, membranaceous ; rachis winged; pinnules alter- 
 nate almost simple, broad at the base, becoming regularly narrower at each lobe, so as 
 * Ann. and Mag. Nat. Hist., 1847, xx., t. 11, f. 2. 
 
 + Pal. Indica (Gondwana Flora), 1879, Ser. xii., No. 1, t. 14a, bis., f. 1, la, and 2. } 
 + Handbook Queensland Geol., p. 63. 
 
367 
 
 to form an almost conical leaflet, emerging at an open angle and curving upward, the 
 lower shorter, the upper longer and spreading; lobes linear, narrow, rounded, very 
 slightly segmented, much longer in the upper pinnules, the terminal lobe produced; 
 costa conspicuous, reaching the apex ; veins very fine, emerging at an acute angle, 
 bifurcating immediately, sending a venule to the end of each lobe. (Ten. Woods.) 
 
 Obs. This fern is said to be comparable with the genus Hymenophyllum, but 
 the figure is so frightfully obscure that it becomes difficult to make anything of it. 
 
 Loc. Rosewood, near Ipswich (The late Rev. J. HE. T. Woods; Macleay 
 Museum, University of Sydney). 
 
 Genus—TRICHOMANITES, Goeppert, 1836. 
 (Syst. Fil. Foss., p. 174.) 
 
 TRICHOMANITES LAXUM, Ten. Woods, ? Pl. 18, fig. 9 
 
 Trichomanides lacum, Ten. Woods, Proc. R. Soc. N. S. Wales, 1883, viii., Pt. 1, p. 95, t. 10, f. 2. 
 
 Loc. Rosewood, near Ipswich (The late Rev. J. H. Tenison Woods ; Macleay 
 Museum, University of Sydney). 
 
 Occurs also in the Burrum Coal Field, under which head a ed oer will 
 be found. 
 
 TRICHOMANITES SPINIFOLIA, Ten. Woods, Pl. 18, fig. 8. 
 Trichomanides spinifolia, Ten. Woods, Pro. Linn. Soc. N. 8S. Wales, 1883, viii., Pt. 1, p. 95, t. 8, f. 7. 
 
 Sp. Char. Frond somewhat stiff, spreading, dichotomously divided, bi-pinnate, 
 pinne opposite, or nearly so, long, linear, and, together with the rachis, nembranaceously 
 winged; pinnules nearly opposite or alternate, very short and quite acute, the apical 
 one long and linear, veins thick, simple, free. (Zen. Woods.) 
 
 Obs. This fern is distinguished by its rigid aspect, numerous close pinne, and 
 short and acute pinnules, except the terminal one, which is disproportionately linear. 
 (Ten. Woods.) 
 
 The specimens before me, of which PI. 18, fig. 8, may be taken as a good 
 example, are larger and stronger, and the pinnules more spine-like, blunt, and athh 
 They appear to form a link between this species and Z. elongata, Carr., sp. 
 Again, there is a resemblance between the present plants and Hymenophyllites dubia, 
 Curran.* 
 
 Loc. Rosewood, near Ipswich (The late Rev. J. HB: T. Woods; Macleay 
 Museum, University of Sydney); Redbank, near Mount Esk, Brisbane River, north 
 of Laidley (W. Souttar)— Hard, altered, brittle shale. 
 
 TRICHOMANITES ELONGATA, Carruthers, sp. 
 
 Sphenopteris elongata, Carruthers, Quart. Journ. Geol. Soc., 1872, xxviii., p. 355, t. 27, f. 1. 
 Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. 1, p. 92. 
 a “ Feistmantel, Palaeontographica, 1878, Suppl., Bd. iii., Lief 3, Heft 3, p, 108. 
 
 Sp. Char. Frond dichotomously divided, each division irregularly pinnate ; 
 pinne simple, bifurcate, or irregularly pinnate; segments narrow, linear, slightly 
 tapering upwards to the rather blunt apex; the single midrib sending out simple 
 branches, which run along the middle of each segment. (Carruthers.) 
 
 Obs. This species is said by Mr. Carruthers to be an abundant fern, but the 
 Rey. J. E. T. Woods casts some doubt on this statement. The fern seems to accord 
 much more with Trichomanites than it does with Sphenopteris. 
 
 99 ” 
 
 
 
 * Proc. Linn. Soc. N. S. Wales, 1884, ix., Pt. 2, p. 253, t. 9, f. 1 and 2. 
 
368 
 
 T. elongata would appear to be a less rigid and more laxly growing fern 
 than 7. spinifolia, Woods. The spiniform pinnules are also absent, but specimens 
 conform much more to Woods’ description of the terminal pinnules of his species. 
 A stouter and more rigid-looking variety has been collected by Mr. G. Sweet, at 
 Thomas’s Mine. The midrib is also less distinct and the pinnules are striate. 
 
 Loe. Tivoli Coal Mine, Ipswich (The late R. Daintree) ; the same and Thomas's 
 Aberdare Coal Mine, Ipswich (Lhe late Rev. J. H. T. Woods—Macleay Museum, 
 University of Sydney; G. Sweet—Colln. Sweet, Melbourne). 
 
 Family—NEUROPTERID. 
 
 Genus—THINNFELDIA, Ettingshausen, 1852. 
 (Abhandl. K. K. Geol. Reichsanstalt, i., Abth. 3, No. 3, p. 2.) 
 
 THINNFELDIA ODoNTOPTEROIDES, Morris, sp., Pl. 17, f. 1, and ? Pl. 17, f. 7. 
 
 Pecopteris odontopteroides, Morris, Strzelecki’s Phys. Descrip. N. S. Wales, &¢., 1845, p, 249, t. 6, f. 2-4. 
 
 “Gleichenites odontopteroides, McCoy, Ann. and Mag. Nat. Hist., 1847, xx., p. 147. 
 
 ? Cycadopteris odontopteroides, Schimper, Traité. Pal. Vég., 1869, i., p. 488. 
 
 Alethopteris ? odontopteroides, Schimper, Jbid., p. 569. 
 
 Pecopteris odontopteroides, Carruthers, Quart. Journ. Geol. Soc., 1872, xxviii., p. 355, t. 27, f. 2 and 3. 
 
 Odontopteris odontopteroides, Crépin. Bull. Acad. R. Belgique, 1875, xxxix., p. 258, f. 1-5. 
 
 Thinnfeldia odontopteroides, Feistmantel, Pal. Indica (Gondwana Flora), 1879, i., Pt. 4, p. 201 ; ? Zbzd., 1881, 
 ili., fas. 3, p. 85, t. 23a. f£. 7-9. 
 
 Feistmantel, Palaeontographica, 1878, Suppl. Bd. iii., Lief 3, Heft 3, pp. 89 and 
 105, t. 13, f. 5, t. 14, £. 5, t. 15, £. 3, t. 16, f. 1; Idid., 1879, Heft 4, p. 165, t. 9 
 (27), 11 (29). 
 
 s, aa Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., Pt. 1, p. 103. 
 - “e Curran, Ibid., 1884, ix., Pt. 2, p. 252, t. 9, f. 4. 
 
 Obs. A full description of this characteristic Australian fern will be found in 
 the late Rev. J. E. Tenison Woods’ Memoir, translated from Feistmantel, with an 
 abridgment of the latter’s remarks. The species passes through endless varieties, some 
 of which will no doubt in the future be better for names. This will account for the 
 evident discrepancy which exists between the single figures of various Authors ; 
 but when a series of specimens are assembled from a given locality, at which the fern 
 is found in abundance, it is at onceseen how these diversified forms all graduate one 
 into the other. m 
 
 It was doubtless a very large fern, and some idea of this can be gathered from 
 Pls. 9 (27) and 11 (29) of Dr. Feistmantel’s Memoir, and before me is an example of no 
 mean size, from Bundanba, measuring ten inches in length. From Ipswich we have 
 examples with the pinnules resembling Feistmantel’s Pl. 9 (27), fig. 1, but of rather 
 smaller growth. From Mount Esk is a good terminal pinnule allied to the right hand 
 of the two figures given on the same Author’s Pl. 10 (28). At Kileoy Range occurs a 
 form with the square step-like pinnules resembling Mr. Carruthers’ figure ; and, lastly, 
 from Petrie’s Quarry, Brisbane, we have a specimen bearing a strong resemblance to 
 Morris’s original figure in Strzelecki’s work (t 6, f. 4). 
 
 In Queensland, Lhinnfeldia would appear to occupy a relatively higher position 
 than it does in New South Wales. I am not aware of its occurrence below the Hawkes- 
 bury Series in the latter Province, but in Queensland it seems to be characteristic of one 
 or more higher horizons. 
 
 The nearest allies are, according to Dr. Feistmantel, 7. swbtrigona, Feist., in 
 the Mesozoic rocks of India, and Z. erassinervis, Geinitz, in similar rocks of the Argentine 
 Republic. 
 
869 
 
 In Pl. 17, fig. 7, is a fern, the right-hand pinnules of which agree with those of 
 TL. odontopteroides, whilst those on the left agree better with those of Z. media, Ten. 
 Woods, or even the var. falcata, and seems to represent a transition form between the 
 two species (?). 
 
 In his Memoir on the Australian Coal Flora, Mr. Tenison Woods mentioned, 
 amongst the fossils of the Ipswich Basin, Thinnfeldia australis, but he does not describe 
 such a species. 
 
 Loc. New Chum, Bundanba, Ipswich Basin, 170 ft. below New Chum Upper Seam, 
 Pl. 17, f. 1 (R. C. Ringrose) ; Redbank, near Mount Esk, Brisbane River, north of 
 Laidley (W. Souttar); Kaleoy Range, above Cressbrook (W. Souttar); Tivoli Mine, 
 Ipswich (G. Sweet—Colln. Sweet, Melbourne). 
 
 _ In addition to these localities, the Macleay Museum contains specimens collected 
 by the late Rev. J. E. T. Woods, and not mentioned in his Paper, from—Aberdare 
 Mine, Ipswich; Rosewood Scrub, near Ipswich; and Pine Mountain, Moreton 
 District. 
 
 THINNFELDIA ODONTOPTEROIDES, vav. FALCATA, Zen. Woods. 
 
 Thinnfeldia odontopteroides, var. falcata, Ten. Woods, Proc. Linn. Soc. N, 8S. Wales, 1883, viii., Pt. 1 
 (> UO ts teh) tinal 
 
 Obs. Proposed as a variety for that form of Z. odontopteroides in which the 
 habit was stouter, and probably not so large in growth. The rachis is always grooved 
 and more slender, and in some specimens the terminal pinnules form a long lanceolate 
 pair. ; 
 The ferns from Petrie’s Quarry, in my Colleague’s Collection, and identified by 
 ' Mr. R. Kidston as this variety, to some extent resemble it, but the pinnules are hardly 
 decurrent or falcate enough. Mr. Woods, however, says that they become long and 
 faleate as they ascend the rachis, and this is so far borne out by our specimens, in that 
 the upper pinnules are much longer and lanceolate than the lower, the latter retaining 
 more of their normal wedge-deltoid outline. 
 
 Closely allied to this variety, in all probability, is that denominated var. lancifolia — 
 by Morris,* and which would appear to have been refigured by Feistmantel + without 
 remark, from another specimen. Now the plants from Petrie’s Quarry have the 
 upper pinnules shaped like those of var. lancifolia, but with the lower ones as above 
 described, and taking upon themselves the more exact outline of Z. odontopteroides. 
 One or two are even slightly falcate. 
 
 Loc. Rosewood, near Ipswich (The late Rev. J. LZ. T. Woods—Macleay Museum, 
 University of Sydney) ; Petrie’s Quarry, near Brisbane (R. C. Ringrose). 
 
 THINNFELDIA MEDIA, Ten. Woods ? 
 
 Pl. 17, fig: 2, Pl. 18, fig. 10 (compare Pl. 17, £. 7): 
 
 Obs. For description of the species, see under ‘“‘ Burrum Beds.”’ 
 
 Loc. Rosewood, near Ipswich (Rev. J. H. TL. Woods—Macleay Museum, 
 University of Sydney) ; Colinton, Upper Brisbane River, Pl. 18, fig. 10 (Hon. A. C. 
 Gregory) ; Tivoli Coal Mine (@. Sweet—Colln. Sweet, Melbourne). Occurs also in the 
 Burrum Beds. 
 
 
 
 * Phys. Descrip. N. 8. Wales, &c., 1845, p. xvi., t. 6, f. 4 
 + Palaeontographica, Suppl. Bd. iii., 1878, Lief. 3, Heft 3, t. 15, f. 4, 
 
370 
 Family—PECOPTERID. 
 
 Genus—ALETHOPTERIS, Sternberg, 1826. 
 (Flora der Vorwelt, Heft 4, p. xxi.) 
 
 ALETHOPTERIS AUSTRALIS, Morris, sp., Pl. 16, fig. 1. 
 
 Obs. For description of the species, see “ Burrum Beds.” 
 
 Loc. New Chum, Bundanba, Ipswich Basin, fifty feet above the second seam 
 (R. Archibald); Gray’s Seam, Ipswich (R. Archibald) ; Kileoy Range, above Creswick * 
 (W. Souttar) ; Colinton, Upper Brisbane River, Pl. 16, fig. 1 (Hon. A. C. Gregory) ; 
 six miles north of Esk, forty-six miles west-north-west of Ipswich (W. Souttar— 
 Mining and Geol. Museum, Sydney); Rosewood, near Ipswich; Peak Mountain, 
 Moreton District; and Fassifern (Zhe late Rev. J. HL. Tenison Woods—Macleay 
 Museum, University of Sydney); Stewart’s Creek, Stanwell (Zhe late James 
 Smith). 
 The plant bed at the last locality consists of a decomposed earthy ironstone, 
 chiefly composed of Teniopteris and the pinnules of a Pecopteroid fern. Several of 
 these have the precise venation of Alethopteris australis, and I think we must accept 
 this as an additional locality for this species. Alethopteris australis occurs also in the 
 Burrum Coal Measures. 
 
 ALETHOPTERIS LinpLEYANA (Royle) Feistmantel, Pl. 17, figs. 3 and 4. 
 
 Alethopteris Lindleyana Feistmantel, Palaeontographica, Suppl. Bd. iii., 1878, Lief 3, Heft 3, t. 18, f. 10. 
 “0 Lindleyana, Feistmantel, Pal. Indica (Gondwana Flora), 1881, iii., Pt. 3, p. 80, t. 18a, f. 2 and 
 2a, t, 19a, £. 3 and 4, t. 23a, f. 11,'t. 39a, ft. 10.and 1, 
 
 Obs. The small specimen figured (Pl. 17, figs. 3 and 4) .is believed both by Mr. 
 Kidston and myself to be identical with Feistmantel’s representation of Alethopteris 
 LIindleyana, Royle; at any rate it is indistinguishable from his earlier figure. Further- 
 more, there is a considerable general resemblance to Tenison Woods’ representation of 
 Merianopteris major, Feistmantel, but in the specimens before me the basal secondary 
 veins do not diverge from the primary vein or midrib in any way different from that 
 usually met with in Alethopteris, and certainly not possessing the outward sweep charac- 
 teristic of Merianopteris. It naturally follows that in many Alethopteroid ferns there 
 must be a greater or less resemblance to the vein-arrangement of Merianopteris. The 
 resemblance will much depend on the degree to which the pinnulesare incised, or cut up. 
 In some cases, and even in the same specimens, the pinnules may be divided almost to 
 the pinna rachis, leaving only so much of their surface confluent as to constitute one 
 of the generic characters. This is apparent in the above figure. When, however, the 
 division between the pinnules is only marginal, or but partial, some of the basal veinlets 
 of contiguous lobes appear in apposition, and in such cases the fern is likely to be 
 mistaken for a Merianopteris. Such an appearance is, in reality, widely different from the 
 structure represented in Feistmantel’s figures of JZ. majort+ where the two lower 
 veinlets on each side a pinnule are arched outwards, and in an otherwise clear space 
 devoid of veins, the latter being crowded together towards the apices.. 
 
 Loe. Redbank, near Mount Esk, Brisbane River, north of Laidley 
 (W. Souttar). 
 
 * Determined by Mr. R. Kidston. 
 + Pal, Indica (Gondwana Flora), 1881, iii., Pt. 3, t. 19a, f. 9-11. 
 
7. 
 
 871 
 Family—GLEICHENIACES, 
 
 Genus—GLEICHENTA, Smith, 1791. 
 (Mém,. Acad, Turin, v., p. 418. 
 
 GLEICHENIA LINEATA, Zen. Woods. 
 Gleichenia lineata, Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. 1, p. 180, t. 3, f. 6, t. 8, f. 2. 
 
 Sp. Char. Frond small, coriaceous, with a strong thick rachis, dichotomously 
 divided, pinnate, bi-pinnate. Pinnules entire, linear, attached by almost the whole of 
 the base, but slightly contracted at the lower portion, somewhat distant, not decurrent. 
 Upper edge convex; lower slightly concavé, but in a few pinnules divided into deep 
 rounded lobes, apex acute, emerging from the rachis at an angle of about 35°, veins not 
 prominent, coste not forking, and quite persistent to the apex, not very visible in any 
 of the specimens, but apparently grouped and numerous, emerging at an acute angle, 
 and bifurcating ; there appear to be two venules emerging at the very base of the 
 pinnule. Rachis conspicuously marked with a single deep, dark, median groove. (Zen. 
 Woods.) 
 
 Obs. This is said to be closely allied to the recent Gletchenia flabellata, 
 R. Brown, common to the east coast of Australia. The Author thinks that perhaps 
 the deep rounded lobes may be a monstrosity. I have not met with the species in my 
 Colleague’s gatherings. 
 
 Loc. Rosewood, near Ipswich (The late Rev. J. H, T. Woods—Macleay Museum, 
 University of Sydney). 
 
 Family—TANIOPTERIDA. 
 
 Genus—TAANIOPTERIS, Brongniart, 1828.* 
 (Prod. Hist. Vég. Foss., p. 61.) 
 
 TmNIOPTERIS (P ANGIOPTERIDIUM) DatnrrReEeEr, McCoy. 
 
 Teniopteris Daintree’, McCoy, Trans. R. Soc. Vict., 1860, v., pp. 196 and 215. 
 re McCoy, Geol. Survey Vict., Dec. ii., 1875, p. 15, t. 14, f. 1 and 2, 
 Feistmantel, Palaeontographica, 1878, Suppl. Bd. iii., Lief. 3, Heft 3, p, 110, t. 14, 
 f. 2and 3; Ibid. 1879, Heft. 4, p. 169, t. 12, f. 5. 
 ‘S Ten. Woods, Proc. Linn. Soc. N.S. Wales, 1883, viii., Pt. 1, p. 117. 
 
 Sp. Char. Frond very long, narrow, strap-shaped, elongately lingual, petiolate, 
 straight, slightly curved, or rather flexuous, parallel-sided, or the margins undulating, or 
 gently sinuous in places, with an average width of five-sixteenths of an inch. Apex 
 rounded, acute, or emarginate. Petiole strong, striated, and naked. Midrib, or costa, 
 thick, striated longitudinally, retaining its size throughout the length of the frond; 
 veins distant or close, simple, or bifureate, generally at right angles to the midrib, but at 
 times slightly oblique, without curve, dichotomisation taking place near the midrib, or at 
 a variable distance between it and the margin. 
 
 Obs. Ihave been, for some time past, accumulating material, with the view of 
 assisting in the identification of some fragmentary Tniopterid remains from Queens- 
 land. YL. Daintreei was first recognised as a Northern form by Dr. O. Feistmantel, from 
 the Talgai Diggings. I have been favoured from time to time with a Teniopteris from 
 Stewart’s Creek, near Stanwell, where the matrix is almost wholly composed of 
 fragments, by my Colleague; from the Peak Mountain, Moreton District, by 
 the late Rev. J. E. T. Woods; and from Starfield, near Mount Morgan, by 
 Mr..A. J. Vogan. In New South Wales, Z. Daintreei was first recognised in the 
 
 3? 
 
 
 
 
 
 * Restricted, Schimper, Traité Pal, Vég., 1869, i., p. 600. 
 
372 
 
 Clarence Series of Grafton by Mr, E. F. Pittman,* and we now possess a very excellent 
 series of Teniopteris from the Mesozoic Beds of the Talbragar River District.t More 
 recently the late Mr. C. 8S. Wilkinson collected a series of specimens at Mylne’s Gap, 
 about twenty-five miles north-west of Grafton. The identity of the Talbragar River 
 specimens with the typical 7. Daintreei in the National Museum, Melbourne, has been 
 obligingly confirmed by Prof. McCoy, to whom specimens were sent. 
 
 The determination of the united Queensland and Clarence River examples has 
 given me a great deal of trouble, from their fragmentary condition, and variability of 
 characters. Notwithstanding the opinion of Pro? McCoy, to whom specimens were 
 also sent, that these “ are specifically distinct from 7. Daintreei,” I have provisionally 
 united these leaves with that species for the following pore ieee an similarity in the 
 growth and form of the frond ; (6) identity in the nature of the venation in all but one 
 point ; and (c) absence of other negative characters. 
 
 The frond of Z. Daintreei attained some size, one specimen from the Talbragar 
 River measuring seven inches in length (and then not perfect) by eight-sixteenths of an 
 inch wide. Prof. McCoy states that he had never seen a specimen of this fern 
 more than about four lines wide, but, as individual fronds reached as much as four 
 inches long, it must “ have been of a singularly narrow, long, linear shape.’ It most 
 resembles the English Oolitic 7. vittata, Phill., but is smaller, very much narrower, 
 and thicker than the latter. All seen by me are separate and detached leaves, no 
 trace of a pinnate arrangement having presented itself, but the general resemblance 
 to those species possessing this character, and for which Schimper proposed the 
 genus Angiopteridium, is so strong, that one is insensibly led to refer the present 
 species to it. 
 
 The petiole was long and strong, the frond insensibly expanding in width 
 upwards from it, describing either a straight, curved, or flexuose course. In the 
 majority of instances the margin is entire, and the frond in consequence parallel-sided, 
 but examples are before me in which the edges are irregularly emarginate, producing 
 at times almost fantastic outlines. In specimens from the Talbragar River the apices 
 are either rounded or acute, generally the former; but in Queensland examples the 
 rounded apices are sometimes emarginate centrally. These blunt’ rounded apices are 
 precisely similar to Oldham and Morris’s, fig. 5,f and to that of Nathorst’s 7. (Olean- 
 dridium) obtusa.§ 
 
 The direction of the veins in the Talbragar examples, on passing from the midrib 
 is, as described by McCoy, at right angles, but here and there a specimen is met with in 
 which the veins break from the midrib at a decided angle. The bifurcation of the veins 
 into venules is very variable, and does not seem to follow any general rule. It may take 
 place close to the midrib, halfway between the latter and the margin of the frond, or 
 near the last-named. 
 
 Whether we take the Clarence River or Queensland specimens, the form and 
 proportions of the fronds are the same, and the venation and its bifureation are of a similar 
 character, but here there is great variation in the angle of divergence of the veins from 
 the midrib. These discrepancies, however, are all to be seen on one and the same specimen. 
 Thus: some veins are quite at right angles, as in a typical 7. Daintreei from Victoria, 
 and the Talbragar River examples; others, a few lines away, are inclined upwards ; 
 
 * Ann. Report Dept. Mines N. 8. Wales for 1879 [1880], p. 227. 
 
 + Ann. Report Dept. Mines N. 8. Wales, for 1889 [1890], p. 287. 
 
 t Pal. Indica (Gondwana Flora), 1863, i., Pt. 1, fase. 5, t. 6. 
 
 § Flor. Skones Kolforande Bilningar, i., "1878, Haft 1, t. 8, f. 10 and 13 (Sveriges Geol. Undersbniee 
 Ser, C., No, 27). 
 
373 
 
 and again, here and there, a little downwards. From these facts I am inclined to 
 regard such differences simply as the result of pressure or fossilisation, and, in the 
 absence of other negative evidence, to look upon the whole as one variable species. On 
 the other hand, if, following the valued opinion of Prof. McCoy, we regard the 
 Queensland and Clarence River Zeniopteris as distinct from the Talbragar and Vic- 
 torian form, the former can hardly be separated from Angiopteridium spathulatum, 
 McClelland,* a plant possessing fronds of similar size to ours, and a similar variability 
 of venation. Indeed Dr. O. Feistmantel has already remarked on the similarity of 
 this plant to 7. Daintreet. If future researches should warrant a separation of these 
 various fronds into two species, the only possible characters upon which such a 
 division can be made are the somewhat thicker midrib, and slightly wider-apart 
 venation, characters which are most strongly marked in the examples from Peak 
 - Mountain, Moreton District. But here, again, we are met by the Clarence River fronds, 
 which are intermediate between this condition and that of the Talbragar and Victorian 
 forms. 
 
 With the above exception, the contiguity of the veins to one another in the 
 Queensland examples is fairly constant, there being three veins in the space of one 
 millimetre, as a general rule. Most of the specimens are fragments, but one or two 
 examples observed measure three and a-half and five inches in length. The breadth 
 varies, of course, according to the part of the frond measured, but basal portions have 
 been found to be as much as thirteen millimetres wide, whilst higher parts of the 
 frond are five in breadth, and at the apices immediately below the tip about three 
 millimetres. 
 
 The distal ends or apices of the Queensland fronds are very rare, but in two 
 instances observed the terminations taper very gradually to pointed apices, but without 
 being acute. 
 
 As in 2. Daintreei, so here, some of the veins bifurcate, others do not; when 
 division takes place it is either immediately at the midrib or at about half the distance 
 between it and the margin. In some few cases bifurcation is almost marginal. 
 
 The whole of our specimens oscillate between ZL. (Angiopteridium) Daintreei, 
 McCoy, and 7. spathulata, McClelland, with very strong affinity to the latter, 
 and it even becomes a question if the species be not identical. Speaking of 
 these ferns, Feistmantel remarks: ‘“ Of foreign forms the Australian Zenopteris 
 Daintreeit, McCoy, can, to a certain extent, be compared with this Indian form; but 
 the veins in the former seem to be still straighter and are thicker than in our species.” + 
 The latter part of this sentence exactly expresses the difference which exists between 
 the Queensland fossils and McCoy’s species, as well as between the latter and 
 the Indian plant. It will not, however, surprise me if these species have to be 
 united ; if not, most of the Queensland fronds will have to be referred to A. spathulatum, 
 McClelland. 
 
 Loc. Talgai Diggings, Condamine River (Dr. O. Feistmantel—Mining and 
 Geol. Museum, Sydney); Stewart’s Creek, Stanwell, near Rockhampton (R. L. 
 Jack); Rosewood, near Ipswich (Hon. A. C. Gregory); Starfield, near Mount 
 Morgan (4. J. Vogan—Mining and Geol. Museum, Sydney); Peak Mountain, 
 Moreton District (The late Rev. J. H. T. Woods—Macleay Museum, University of 
 Sydney). 
 
 T. Daintreei occurs also in the Styx Coal Field (Burrum Formation). 
 
 
 
 * Oldham and Morris, Pal. Indica (Gondwana Flora), 1863, i., Pt. 1, fas. 6, p. 34, t. 6, f. 1-73 
 Feistmantel, Jbid., Pt. 2, 1877, p. 96. 
 t+ Pal. Indica (Gondwana Flora), 1879, i., Pt. 4, p. 207 
 
374 
 TxNroprenrts (P ANGIOPTERIDIUM) CarruruERs!, Ten. Woods. 
 
 Tewiopteris Daintreet, Carruthers, Quart. Journ, Geol. Soc., 1872, xxvili., p. 355, t. 27, f. 6. 
 ” 7 Feistmantel, Palaeontographica, 1878, Suppl. Bd., iii., Lief. 3, Heft 3, t. 14, f. 4 
 (excl. figs. 2 and 38). 
 ny} Carrutherst, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viil., Pt. 1, p. 117, 
 
 Sp. Ohar. Frond simple (?), broad-linear, cost somewhat thick, veins leaving 
 it at an acute angle, then passing out at right angles to the margin, once or twice 
 dichotomously divided. (Zen. Woods.) 
 
 Obs. This isa larger plant than the original 7. Daintreei of McCoy, and the 
 general form is different. The veins, instead of leaving the midrib direct at right 
 angles, as in the case of the species named, pass from it at first obliquely, and then 
 assume a similar course to the former. These points were used by the Rev. J. E. T. 
 Woods for the separation of this plant from 7. Daintreei, McCoy. 
 
 It is, however, but due to Prof. Sir F. McCoy to state that he appears to have 
 been the first to point out * the difference between the two species, an opinion in which 
 he was supported on three separate occasions by Dr. Feistmantel.t I point this out 
 because the Rev. Mr. Woods appears to have ascribed this matter to the latter observer, 
 although it1s of course possible that Dr. Feistmantel may have independently arrived 
 at sucha conclusion. The great width of the frond, and the comparatively narrow 
 midrib are striking features in this species, and should, with the venation, always serve 
 to distinguish it. It should be distinctly borne in mind that veins leave the midrib at 
 an acute angle, and then inmediately proceed towards the margins horizontally, or at 
 right angles, like those of 7. Daintreei. At least this is Mr. Woods’ statement, but I 
 would observe that in Mr. Carruthers’ figure the veins do not diverge at aright angle 
 after leaving the midrib, but. at one rather more acute than this, although less than 
 that by oie they at first issue from the midrib. 
 
 Teoniopteris Carruthersi is remarkably like Angiopteridium Maclellandi, Old. 
 and Morris, and seems only to possess a wider frond and thicker midrib. 
 
 The Geological Survey Collection contains a single leaflet from the Stewart's 
 Creek Beds which partakes in part of the characters of both the species, and I am quite at 
 a lossto which to refer it. The specimen possesses the form of 7. Carruthersi, and the 
 more numerous and widely diverging veins of dA. Macclellandi, but I have provisionally 
 referred it to the former, 
 
 In Pl. 16, fig. 4, we have a large Teniopteris, at present undetermined, and 
 unfortunately a single specimen. The veins have been drawn as anastomosing, but in 
 reality this is not the case, they simply fork. The leaflet is too large, and the veins 
 too close together for A. spathulatum, neither does it correspond with Z. Carru- 
 therst. Mr. Kidston suggested a reference to A. Jfacclellandi, relying on Zeiller’s 
 figure of the plant from Tonkin,§ but this does not correspond with the original 
 illustration of Oldham and Morris. The specimen must for the present remain 
 unnamed. 
 
 Loc. Tivoli Coal Mine, Ipswich (The late R. Daintree)—Redbank, near Mount 
 Esk, Brisbane River, north of Laidley, Pl. 16, fig. 4 (W. Souttar). See also under 
 Stewart’s Creek Beds, Rockhampton. 
 
 * Geol. Surv. Vict., Dec. ii., 1875, p. 16. 
 
 + Pal. Indica (Gondwana Flora), 1879, i., fas. 4, p. 207; Journ. R. Soc. N. S. Wales for 1880 [1881]., 
 p. 114; Palaeontographica, loc. cit., Heft 3, p. 110. 
 
 t Pal. Indica (Gondwana Flora), 1863, Pt. 1, fas. 5, p. 33, t. 23. 
 
 § Ann. des Mines, 1882, ii., t. 10, f. 5. 
 
375 
 
 Genus—ANGIOPTERIDIUM, Schimper, 1869. 
 (Traité Pal. Vég., i., p. 602.) 
 
 ANGIOPTERIDIUM, sp. ind. 
 ‘Angiopteridium ensis, Ten. Woods (non Oldham and Morris), Proc. Linn. Soc. N.S. Wales, 1883, viii., Pt. 1, 
 p. 119. . 
 
 Obs. The fossil identified by the late Rey. J. E. Tenison Woods with the above 
 species does not appear to accord either with the description or figure of Messrs. Oldham 
 and Morris. In the first place, the Rev. Author’s diagnosis and remarks (the first two 
 paragraphs of his observations on this species), which are presumedly made on his 
 Australian specimens, are, with one or two trivial alterations, copied verbatim from 
 Oldham and Morris, and do not apply in the least degree to the latter. 
 
 The original specimens, now in the Macleay Museum, at the Sydney University, 
 were obligingly lent to me by the late Prof. William J. Stephens. 
 
 The fronds are long and narrow, nearly three inches, and that without being 
 perfect, ribbon-like, or linear-lingual, hardly tapering, and parallel-sided. The midrib 
 is wide and flattened. The veins are very distinct, wide apart, very oblique to the mid- 
 rib, and very little curved, being almost straight. They bifurcate at about one-third 
 from the midrib. The veins do not fork particularly near the margin, and the latter is 
 not in any way serrated ; the former, measured along the margin, are about one millimetre 
 apart. 
 
 The outline of the frond is much more that of Angiopteridium spathulatum, but the 
 venation is wholly different. I have not succeeded in identifying this fern with the 
 limited bibliography at my command, but in the event of its being undescribed I propose 
 to name it A. Tenison- Woodst. 
 
 Loe. Rosewood, near Ipswich (The late Rev. J. EH. 7. Woods—Macleay Museum, 
 University of Sydney). 
 
 Genus—PHYLLOPTERIS, Saporta, 1873. 
 (Pal. Frang., Plantes Jurassiques, i., p. 448.) 
 
 Paytiorrerts FEIStMANTELI, sp. nov. 
 
 Sp. Char. Frond, or leaflet, oval, or broadly lanceolate, slightly petiolate ; mid- 
 rib very distinct, evanescing towards the apex of the leaflet, but tapering very slowly ; 
 veins springing outwards from the midrib at a very acute angle, then gracefully 
 curving outwards to the margin, fine, once or twice furcate. 
 
 Obs. The form of the leaflet appears to be constant and characteristic, those 
 from Queensland and South Australia agreeing closely. The veins bifurcate first near 
 the midrib, and either proceed in this form to the margin, or again divide at about half 
 the distance between the latter and the midrib. Near the apex the midrib evanesces 
 into a few distributed veins. Phyllopteris Feistmanteli is very distinct from Saporta’s 
 type, P. plumula,* both in the form of the leaflet, and from the many times dichoto- 
 mising veins of the latter. 
 
 The species is named in honour of the late Dr. Ottokar Feistmantel, formerly 
 Palzontologist to the Geological Survey of India. 
 
 At first sight, and when superficially examined, the frond might be taken for 
 a Glossopteris ; in fact, I had them sent to me by Collectors from Queensland as such. 
 The venation of Glossopteris is of the well-known reticulate type, that of Phyllopteris 
 is simply furcate; the one being a member of the family Dictyoteniopteride, the 
 other of the Tniopteride. 
 
 * Pal. Frang., Plantes Jurassiques, 1873, i., p. 450, t, 63, f. 6. 
 
376 
 
 The genus Phyllopteris is an old one of Brongniart’s resuscitated by Count 
 Saporta * for a plant from the Ammonites angulatus zone of the Infra-Lias of the 
 Moselle, France. The portions of fronds from the localities below so thoroughly corres- 
 pond with the structure of Phyllopteris, as described by Saporta, that I have adopted 
 it in the sense of the latter. 
 
 The relation of Phyllopteris to other Terrontereee is a very close one, especially 
 those with obliquely curved veins, such as Angiopteridium. In the absence of fructi- 
 fication, or the system of branching, it is somewhat difficult to indicate the difference in 
 words, but the fronds in question certainly do not possess the strap-shaped outlines of 
 many Teniopteris, nor the more or less flabellate appearance of Macroteniopteris, but 
 approach nearest to the first-named genus Angiopteridium. As, however, the full frond 
 in the latter genus is known to be pinnate with marginal sori, and as nothing whatever is 
 known of these characters in the Queensland and South Australian plant, it will be 
 better for the present to retain it in Phyllopteris. 
 
 Loe. Stewart's Creek, Stanwell, near Rockhampton (#. ZL. Jack); Styx River 
 Coal Shaft, Styx River, Broadsound (The late James Smith). I have also received this 
 plant, through the good offices of Mr. H. Y. Lyell Brown, Government Geologist of 
 South Australia, from Cooper’s Creek, Central Australia, about one hundred miles due 
 north of the Leigh’s Creek Bore. 
 
 Genus—MACROTHANIOPTERIS, Schimper, 1869. 
 (Traité Pal. Vég., i., p. 610.) 
 
 MAcRoTHNIOPTERIS WIANAMATTH, Heistmantel. 
 
 Macroteniopteris wianamatte, Feistmantel, Palaeontographica, Suppl. Bd. iii., 1878, Lief. 3, Heft 3, p. 107, 
 to 13, fe, 
 aa =r Ten. Woods, Proc. Linn. Soc. N. 8S. Wales, 1883, viii., Pt. 1, p. 118, t. 10a. 
 
 Sp. Char. Frond elongately obovate, simple; base attenuate; apex?; midrib 
 thick, grooved, or striated; veins emerging at angle of 20°-25° close, near the midrib 
 from six to eight-tenths of a millimetre apart, slender, dichotomous towards the 
 margin. (Zen. Woods.) 
 
 Obs. The late Rev. J. E. Tenison Woods recorded this fern from Ipswich, 
 but added that the dichotomy of the veins is near the rachis, and suggested that in 
 consequence it might be a new species. The presumption is, of course, that the veins 
 divide nearer the midrib than do those in Feistmantel’s type, but on consulting the 
 latter’s figure, it will be noticed that subdivision takes places at various distances 
 between the margin and the midrib. This separation will hardly, therefore, hold good. 
 
 Loc. Ipswich (Lhe late Rev. J. H. Tenison Woods—Macleay Museum, 
 University of Sydney). 
 
 MAcROTANIOPTERIS CRASSINERVIS, Heistmantel ? Pl. 16, fig. 5 
 
 Macroteniopteris crassinervis, Feistmantel, Pal, Indica (Gondwana Flora), 1877, i, Pt. 2, p. 102, t. 38, £. 1-3. 
 Sp. Char. Frond very large, single, strong, thick, and coriaceous, broad, 
 elongately obovate; margins plain; apex obtusely rounded, not re-entrant; midrib 
 distinct, but not wide for the size of the frond, vertically ridged; veins, except near 
 the apex, diverging at a right angle, or nearly so, very strong; distant from one to 
 one and a-half millimetres apart, very regular and direct in their course, simple or 
 forked; dichotomisation at irregular intervals, but always dividing close to the midrib. 
 Obs. I have ventured to refer this noble frond to Feistmantel’s Macroteniopteris 
 “rassinervis, from its coarse nervation, and the uniform manner in which the veins 
 re nie gk tal Wd tc ad le pe eee. ee a 
 
 * Pal. Frang,,-Plantes Jurassiques, 1878, i., p. 448. 
 
377 
 
 divide close to the midrib. The Author remarks of his species—‘ The chief character, 
 however, lies in the secondary veins; they were not numerous, and somewhat distant 
 from each other, showing regular intervals.” The number, of course, depends upon the 
 size of the frond, but otherwise these remarks quite coincide with the characters of our 
 frond. I am unable to make a closer comparison than with the above species, but 
 Feistmantel remarks that JL crassinervis “was of no very large size.” Herein lies a 
 marked departure from our fern, and may perhaps constitute a difference, in which case 
 I should feel disposed to regard this as undescribed, at any rate so far as Australian 
 species are concerned. 
 
 As preserved, the frond is fifteen inches in length, and, if perfect, would measure 
 fully five in breadth. Want of space does not enable me to figure this fine fossil, but 
 the apical portion of a second specimen on the same slab of stone is given (Pl. 16, 
 fig. 5). As regards size, the only species with which it is in my power to compare it is 
 MM. lata, O. and M.,* but here the frond is very delicate, and the veins fine and close, 
 producing a far more tender leaf than that under consideration. 
 
 The veins in the Australian specimen are fully one millimetre apart, and 
 frequently one and a-half. Their regularity is a very marked feature, and the angle 
 of divergence is usually a right angle, or but very slightly removed from it. No rule 
 seems to exist as to the order of subdivision of the veins, but when they are dichotomous 
 the split always takes place in close contiguity to the midrib. It is only towards the 
 apex that the divergence assumes another angle, and then it is much more acute. The 
 apex of the frond is shown in a second specimen, about six inches long, on the same slab. 
 It is obtuse, but at the termination of the midrib sub-mucronate. Two and a-half 
 inches from the apex the width of the frond is three inches. 
 
 Loc. Wycarbah, near Rockhampton (Zhe late James Smith). 
 
 MacroreNoPreris, sp. 
 
 Obs. A portion of a frond which was originally at least four inches wide, generally 
 resembles that of IZ. wianamatte, Feistm. On emerging from the midrib, or costa, 
 the veins are strong and about one thirty-second of an inch apart, but after bifurcation 
 they become exceedingly fine and close together. The subdivision takes place near 
 the rachis, and in this it differs from the species above named, in which bifurcation is 
 much nearer the margin of the pinnule. The late Rev. J. E. Tenison Woods remarked, 
 when speaking of IZ. wianamatte, ‘‘I have some similar specimens near Ipswich, but 
 the dichotomy of the veins is near the rachis, and it may be a distinct species.’’ I take 
 it that the present fossil is a similar one to that mentioned by the Reverend Author, and 
 if 1t should prove distinct, as I anticipate it will, it may be known as DMacroteniopteris 
 Woodst. An early opportunity will be taken to figure this interesting plant. 
 
 Loc. Tivoli Coal Mine, Ipswich (G. Sweet—Colln. Sweet, Melbourne). 
 
 Genus—SAGHNOPTERIS, Presl. 
 (Sternberg’s Flora der Vorwelt, ii.+) 
 
 SAGENOPTERIS RHOIFOLIA (Presl.), Keistmantel. 
 
 Sagenopteris rhoifolia (Presl.) Feistmantel, Palaeontographica, 1879, Suppl. Bd. iii., Lief. 3 Heft 4, p. 170, 
 t. 30, f. 1-4 and 7. 
 A ¥ Ton. Woods, Proc. Linn, Soc. N. S. Wales, 1883, viii., Pt. i., p. 128, t. 9, f. 4. 
 Sp. Char. Frond very variable both as to shape and size; pinne narrow at the 
 base, articulate, spathulate, obovate, or oblong-acuminate, rarely oblong-lanceolate or 
 
 
 
 * Pal. Indica (Gondwana Flora), 1863, i., Pt. 1, fas. 6, t. 1, t. 2, f.1,t.4, land 2, t. 5, &. 
 + Fide Schimper, Traité Pal. Vég., i, p G41. 
 
378 
 
 subrotundate, inequilateral, very rarely subsymmetrical, the middle leaves larger than 
 the lateral ones, and quite entire. Ordinary length about thirty-two millimetres, with 
 a diameter of sixteen millimetres. The internal margins of the lateral fronds somewhat 
 expanded, furnished here and there with a broad indistinct dental lobe. (Zen. 
 Woods.) 
 
 Obs. I have examined the type specimens used by the late Rev. J. HE. T. Woods, 
 which are very beautifully and distinctly preserved in the ferruginous rock of the 
 Darling Downs deposit. Some specimens in the Australian Museum measure as much 
 as three and three-quarter inches in length. 
 
 Dr. Feistmantel records this species from the Talgai Diggings, but Mr. Woods 
 says, ‘ All Australian specimens are from the Upper or Mesozoic Coal Basins of 
 Ipswich, Queensland, and Jerusalem, Tasmania.” . 
 
 Loc. Talgai Diggings, Condamine River (Dr. O. Feistmantel—Mining and 
 Geol. Museum, Sydney) ; Darling Downs, near Toowoomba (The late Rev. J. H. F. 
 Woods—Macleay Museum, University of Sydney). 
 
 SAGENOPTERIS P CUNEATA, Carruthers, sp. 
 
 Cyclopteris cuneata, Carruthers, Quart. Journ. Geol. Soc., 1872, xxvili., p. 355, t. 27, f. 5. 
 ;; *- Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1888, viii., Pt. 1, p. 109. 
 
 Sp. Char. Pinne entire, generally large, cuneate-triangular, narrowed towards 
 the base, and more or less petiolate-like, and the distal margin obliquely rounded, veins 
 delicate, but distinct and very regular, about one-thirty-secondth of an inch apart, once 
 or twice dichotomously divided, sometimes anastomosing at intervals, and then forming 
 a long narrow oval mesh; no trace of a costa or midrib. 
 
 Obs. Both Dr. Feistmantel and the late Rev. J. E. Tenison Woods were inclined 
 to the belief that the original figure represented but a fragment of a pinna. This, and 
 the anastomosis of the veins, described by Mr. Carruthers, led both Authors to doubt 
 the reference to Cyclopteris, Mr. Woods remarking that “ some fragments of Sagenopteris 
 may resemble it.’”’ 
 
 Mr. George Sweet has obtained a specimen from Tivoli, with a distinctly cuneate- 
 triangular outline, and perfect. Mr. Carruthers describes the veins as ‘“ sometimes 
 anastomosing once in their length near the middle of the pinnex,” but Mr. Sweet’s 
 specimen clearly shows that it took place more frequently than this, and, when present, 
 divided the leaf into an imperfect oval network. I have provisionally placed the species 
 in Sagenopteris, although it does not conform strictly to the characters of that genus. 
 It need not in any way be mistaken for a Glossopteris, the outward curve of the veins, 
 the absence of a midrib, and the paucity of the vein-reticulation quite separating 
 S. ? cuneata from that genus. 
 
 Loc. Tivoli Coal Mine (The late R. Daintree; G. Sweet—Colln. Sweet, 
 Melbourne). 
 
 Family—DICTYOPTERID”. 
 
 Genus—PHLEBOPTERIS, Brongniart,* 1828. 
 (Prod. Hist. Vég. Foss., p. 30.) 
 
 PHLEBOPTERIS ALETHOPTEROIDES, Etheridge fil. 
 
 Phlebopteris alethopteroides, Etheridge fil., Proc. Linn. Soc. N. 8S, Wales, 1888, iii., Pt, 3, p. 1806, t. 38 
 f, land 2; Ibid., 1889, iv., Pt. 3, p. 625. 
 
 Sp. Char. Pinne large, probably elongate. Rachis strong, moderately thick or 
 wide, and longitudinally grooved and ridged. Pinnules lingual, strap-shaped, narrow, 
 
 * Emend. Schimper, Traité Pal. Vég., 1869, i., p. 624. 
 
379 
 very long, parallel-sided, alternate, sub-alternate or opposite, very regular in appearance, 
 and equidistant, markedly confluent. Midrib strong, tapering gradually, and extending 
 to the apices of the pinnules; reticulation small, consisting of elongate, rather 
 irregular scale-like vesicles; veins almost at right angles to the midrib, bifurcating 
 immediately after leaving the reticulation. 
 
 Obs. Amongst a collection of plants in the Australian Museum, from the 
 Tpswich Coal Measures on the Dariing Downs, near Toowoomba, I observed some fairly 
 good specimens of what appeared to be Alethopteris ; but the narrow elongate pinnules, 
 springing horizontally from the rachis, did not allow the plant in question to fit happily 
 into that genus. Close examination of the better-preserved examples, revealed a small 
 and very delicate reticulation, consisting of small, elongate, and irregular vesicles, if I 
 may call them so, lying close to the midrib of each pinnule. The appearance presented 
 by this reticulation is very well shown in Schimper’s figure of Phlebopteris affinis, 
 Schenk.* 
 
 Portions of this fern, which I have called Phlebopteris alethopteroides, are as 
 much as seven inches in length, so that the pinne must have attained a no mean size. 
 Individual pinnules, although imperfect, still measure two and a-half inches in length, 
 their breadth, which is very disproportionate to the length, remaining very uniform. 
 The greatest width I have observed a pinna to attain, and that again imperfect, was 
 four and a-quarter inches. The pinnules are, on an average, from a quarter of 
 an inch to five-sixteenths wide, and are separated from one another by interspaces 
 of about a quarter their width. A good deai of irregularity exists in the manner 
 in which the midribs of the pinnules are given off from opposite sides of the 
 rachis. Some are opposite, others are regularly alternate, many are sub-alternate, and 
 others are even intermediate between these positions. 
 
 The veins are very regular, and given off at an angle which slightly varies from 
 a right angle with the midrib, to one more acute. They bifurcate shortly after leaving 
 the reticulation, and proceed direct to the margin. Along the rachis, on the confluent 
 portions of the pinnules, the veins are longer and much wider apart. 
 
 The rachis is always broad and well marked, being rigid and fluted ; and it may 
 not be uninteresting to note a segmentation of the stem in some of the specimens, and 
 always at the base of the pinnules, but arising only from fracture. 
 
 The regularity and stoutness of the rachis and pinnules give to this fern, 
 especially when not too well preserved, almost the aspect of a Cycad. 
 
 In the form of the network on each side the midrib, our species is much like 
 the figure of P. contigua, L. and H., given by Lyell + under the name of Hemitelites 
 Brownti, Gopp. 
 
 The fructification is shown on aspecimenin the Mining and Geological Museum, 
 Sydney, the position of the sori being similar to that of Brongniart’s P. polypodioides— 
 viz., at the ends of short nervules which do not reach the margin of the pinnules. The 
 fructification in its present state is stellate and occupies a large portion of the pinnule 
 surface, and in its minute structure much resembles that of P. Schowvit, Brong. It 
 would seem that the indusium had in each case burst, leaving the interior of the 
 sori exposed, in which case the sporangia are represented by the small radiating sub- 
 divisions. 
 
 Loe. Darling Downs, near Toowoomba (The late C. H. Hartmann—Australian 
 Museum, Sydney). 
 
 * Loc. ct. “Atlas, t. 39; fig. 15: 
 + Student’s Elements of Geology, 2nd Edition, 1874, p. 337, f. 357. 
 
380 
 
 Section—PHANEROGAMIA. 
 Class—DICcOTYLEDONES. 
 
 Order—CYCADACEE. 
 Family—ZAMIEZ, 
 Genus—PODOZAMITES, F. Braun. 
 
 (Miinster’s Petrefactenkunde, vi., p. 36.*) 
 
 PoDOZAMITES LANCEOLATUS, Lindley and Hutton ? 
 
 Zamia lanecolata, L. and H., Fossil Flora, 1837, iii., t. 194. 
 Podozamites lanceolatus, Teisumentel Pal. Indica (Gondwana Flora), 1877, ii., Pt. 2, p. 11 (91), ae eaves © 
 t. 4, f. 1-10. 
 + a Ten. Woode: Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. i., p. 145. 
 
 Sp. Char. Leaves remote, deciduous, entire, narrowed at base, lanceolate, 
 acuminate at the apex; nerves many, forked just above the base, then simple, and 
 converging to the apex, parallel, from eight to twelve in a leaf. Leaves from forty-five 
 to one hundred millimetres in length, and from two to twelve in breadth, according as 
 the leaf is ovate or lanceolate, (Ten. Woods.) 
 
 Obs. The above is the late Rev. J. E. Tenison Woods’ description of the 
 Australian plant. The determination is open to some doubt, as the Reverend Author 
 seems to have hesitated between P. lanceolatus aud Zeugophyllites elongatus, Morris. 
 Denuding his remarks of quotations from other Authors, he says: ‘‘ Both these varieties 
 (¢.e., the Indian) occur abundantly in the Ipswich Basin, one specimen showing how the 
 leaves were affixed to the parent stem, and, though the fragment is imperfect, it shows 
 precisely the growth figured by Schimper . . . . . . This plant may have been 
 the same as Zeugophyllites australis, Morr. It must be remembered that the latter 
 genus was established by Brongniart for a plant ‘with leaflets such as these, but in 
 pairs.” 
 
 Loc. Ipswich Basin (The late Rev. J. H. T. Woods—Macleay Museum, 
 University of Sydney). 
 
 Popozamitss, sp., Pl. 18, fig. 5 
 
 Obs. Leaflets somewhat similar to those described from “ Burrum, above the 
 Bridge Seam—Hon. W. Walsh”’ (Pl. 18, fig. 4), are presented in this specimen, but 
 larger and displaced with respect to one another. The venation is stronger than in 
 the previous form, and the apices blunter, although that of the larger pinnule does 
 not represent a true margin, but a fractured edge. There are about eight 
 veins in the space of half aninch. This approaches nearest to Podozamites Zeillerianus, 
 Zigno,} an Italian species, both in size and nature of the venation, except that in 
 our plant the veins occasionally bifurcate, whilst in the former they are simple. 
 
 Similar broad pinnules are figured by Schenk, in Richthofen’s “ China,” as 
 Podozamites lanceolatus, var. latifolia. Here,t on the whole, they appear much 
 more finely veined than our Pl. 18, fig. 5, but some have acute apices, as in Pl. 18, 
 fig. 4. 
 
 The questionable occurrence of Zeugophyllites in Queensland rocks has already 
 been referred to under Podozamites lanceolatus. From Mount Esk some long 
 and fragmentary striated and simple leaves have come under notice, which Mr. R. 
 
 
 
 
 
 * Fide Zigno, Flora Foss. Formationis Ool., Vol. ii., p. 118. 
 + Zigno, Flora Foss. Formationis Ool., ii., p. 180, t. 41, f. 1-6. 
 t Beitrage zur Palaontologie von China, 18838, Bd. iv., t. 49, f. 5, t. 50, f. 4, t. 51, f. 6. 
 
381 
 
 Kidston suggested might be those of Zeugophyllites. They are certainly like those of 
 Z. eagapus. Morris, but it seems to me that their length is too great in proportion to 
 their width, and the aces too parallel for a leaf possessing the somewhat tapering 
 outline of the species named. ‘The leaves are striated faintly, and associated with 
 Thinnfeldia odontopteroides, and Teniopteris. These leaves are, I think, much more 
 likely to be those of Podozamites, leaving out of question the relation of the latter and 
 Zeugophyllites. 
 
 Loc. Redbank, near Mount Esk, Brisbane River, north of Laidley (W. Souttar). 
 See remarks on the specimen, Pl. 18, fig. 4, under the head “ Burrum.” 
 
 Genus—OTOZAMITES, F. Braun. 
 (Miinster’s Petrefactenkunde, vi., p. 36.) 
 
 OTOZAMITES MANDESLOHI, Awrr. 
 
 Otozamites (comp. Mandeslohi, Kurr), Feistmantel, Palaeontographica, 1879, Suppl. Bd. iii., Lief 3, Heft 4, 
 De lily t. boot. 
 AE Mandeslohi, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., Pt. 1, p. 151. 
 
 Sp. Char. Leaves long linear, gradually narrowed towards the apex, twenty- 
 five millimetres wide, leaflets densely crowded, oblique, alternating, inserted on the 
 rachis with contiguous bases, ovate, oblong, obtuse, base subcordate, fourteen millimetres 
 long, eight broad; nerves close, diverging. (Zen. Woods.) 
 
 Obs. The Australian plant is believed by Dr. Feistmantel to be identical with 
 
 that from the Lias of Wurtemberg. 
 Loe. Talgai Diggings, Condamine River (Dr. O. Feistmantel—Mining and 
 
 Geol. Museum, Sydney); Darling Downs, near Toowoomba (The late Rev. J. HE. T. 
 Woods—Macleay Museum, University of Sydney; Lhe late OC. H. Hartmann—Aus- 
 tralian Museum, Sydney). 
 
 Genus—PTEROPHYLLUM, Brongniart, 1828. 
 (Prod. Hist. Vég. Foss, p. 95.) 
 
 PTEROPHYLLUM ABNORME, sp. nov., Pl. 17, fig. 5 and 6. 
 
 Sp. Char. Pinne probably long and narrow; pinnules small, narrow, quite 
 parallel-sided, alternate, or sub-alternate, decurrent, attached by their whole bases, 
 generally distinct from one another, but sometimes slightly confluent, not constricted 
 at the base; apices broadly rounded and not in any way acuminated ; veins distinct, 
 about ten at the basal end of pinnules, each bifurcating at about half the length of the 
 leaflet, direct, not converging towards the apex; rachis not very broad, distinct, and 
 longitudinally striate. 
 
 Obs. A few examples of this plant have come under my notice, but all presenting 
 similar characters. Strictly speaking, the dichotomy of the veins would remove the 
 species from Pterophyllum, where they are always described as simple. On the other 
 hand, in those genera in which the simplicity of the venation is lost, the pinnules are either 
 inserted on the rachis by a callosity, as in Zamites ; with an articulated base, as in 
 Otozamites; by an attenuated and articulated base like Podozamites ; or partially united, 
 as in Ptilophyllwm. Inthe present case the pinnules are most certainly decurrent, and 
 for that reason I prefer to provisionally retain the plant in Pterophyllwm. 
 
 In the form of the pinnules and their separation from one another, there is a 
 general resemblance to Pteroph yllum Falconerianum, Morris,* but the fronds of this 
 species are larger, and the veins simple. 
 
 Loe. Redbank, near Mount Esk, Brisbane River, north of Laidley (W. ay 
 
 * Pal, Indica (Gondwana Flora), 1863, i, Pt. 1, fas, 3, t, 14, f. 1. 
 
 
 
382 
 
 PrEROPHYLLUM, sp. ind., Pl. 16, fig. 8. 
 
 Sp. Char. Form of frond unknown. Rachis moderately broad, longitudinally 
 wrinkled. Pinnules long, transversely elongated, parallel-sided, apices unknown, expand- 
 ing slightly towards the base of attachment, in one instance almost confluent, alternate, 
 but moderately contiguous to one another. Veins strong, well-marked, apparently 
 about twenty. 
 
 Obs. A single example, and that fragmentary, does not permit of a species 
 being established, although, so far as Queensland is concerned, there is no doubt this is 
 quite new. 
 
 It appears to partake of the character of P. Falconerianum, Morris.* 
 
 This is not unlike some forms of Zamites, but, although one or two of the bases 
 of the pinnules appear a little thickened, I do not see any trace of a callosity in the 
 sense as applied to that genus. 
 
 Loc. Colinton, Upper Brisbane River (Hon. A. C. Gregory). 
 
 Genus—PTILOPHYLILUM, Morris, 1840. 
 (Trans. Geol. Soc., 1840, v.) 
 
 PriLOPHYLLUM OLIGONEURUM, Ten. Woods. 
 
 PI 18) fie. and 2 PEO. pees, 
 Ptilophyllum oligonewrum, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., Pb. 1, p. 149, t. 7, f. 2-4. 
 
 Sp. Char. Frond pinnate, long linear, gradually tapering to the apex; pinne 
 rather long, narrow, slightly oblique, alternate, separate, but very close, rounded and 
 curved, somewhat falcate, ending in quite an acute apex at the upper edge, base 
 rounder or auriculate above, obliquely inserted, leaving when detached a series of 
 oblique, alternate, elongate depressions on the rachis; veins distinct from their origin, 
 and parallel to the apex, from four to six in number, all well marked and conspicuous. 
 Length of longest pinne twelve to fifteen millimetres, breadth one and a-half to two 
 millimetres. (Ten. Woods.) 
 
 Obs. “Thespecies . . . . partakes of anintermediate character. It has the 
 acute leaflets of P. acutifoliwm and the small size of P. cutchense, and furthermore is 
 distinguished from both by its few, simple parallel veins.” , 
 
 I much question the distinctness of this plant from some varieties of P. acuti- 
 Solium, Morris,t to which in fact Mr. Kidston had referred our specimens. 
 
 Loc. Rosewood, near Rockhampton (The late Rev. J. H. T. Woods—Macleay 
 Museum, University of Sydney); Wycarbah, near Rockhampton (2. L. Jack, and the 
 late James Smith). 
 
 Order—CONIFERE. 
 
 Obs. The following epitome of our knowledge of Australian Fossil Conifers is 
 quoted from the late Rev. J. E. Tenison Woods’ Memoir:—‘ We have abundant 
 evidence of the existence of Conifers in Australia, in almost all our plant beds except 
 the very earliest coal formations.{ This is necessary to bear in mind, because Morris, in 
 Strzelecki’s Work already referred to, lays stress upon the absence of such woods from 
 the New South Wales specimens. Wood, leaves, and scales of conifers are mentioned 
 by Dana. Many specimens of coniferous wood are reported to occur in the Lower 
 
 * Pal. Indica (Gondwana Flora), 1863, i, Pt. 1., fas. 3, t. 16, f. 1. 
 t+ Pal. Indica (Gondwana Flora), 1863, i., Pt. 1, fas. 4, p. 29, t. 20, t. 21, f. 2. 
 t Even this exception need no longer be made. See pp. 49 and 198, 
 
383 
 
 Coal Measures, Greta Creek. Wood and leaves are found in the Jerusalem Coal 
 Basin in Tasmania, and both are common, as we have .scen, in the Ipswich Coal Beds, 
 and in the Tivoli Mines in Queensland. 
 
 “ Fragments of a kind of jet, in which, however, the coniferous structure is very 
 visible, are common also in the Desert Sandstone in Queensland. Finally, there are 
 some fossil Walchia, which evidently bore a large share in forming the coal at 
 Ballimore.” 
 
 The late Mr. James Smith collected coniferous wood at Wycarbah, near Rock- 
 hampton (Pl. 4, figs.9 and 10). Our figures have hardly been enlarged enough to show 
 the complete structure, but in the specimen from which they are taken it is very finely 
 preserved. They are portions of a Cupressinous Conifer, allied to, if not identical with, 
 Spondylostrobus, von Mueller. Pl. 4, fig. 9, is a radial section showing the medullary 
 rays in horizontal lines, and the woody fibres in vertical lines. Fig. 10 is a transverse 
 section, the walls and cavities of the woody fibres shown in quadrangular spaces, but 
 the resin ducts are not visible. The latter, however, Baron von Mueller informs me, 
 are frequently not visible in Spondylostrobus. The Baron has examined these slides 
 and assents to their reference to his genus. Mr. Smith informed me that the block of 
 wood was not found zz sitw at Wycarbah, but, with many others, lay scattered over the 
 surface of some miles of country, and, in fact, that such fragments are common every- 
 where in Central Queensland. From this it is exceedingly doubtful if it belongs to the 
 plant-bearing series at Wycarbah; in fact, the evidence is pretty conclusive that it does 
 not. On the contrary, the wood is probably derived from the denudation of some later 
 formation now swept away. 
 
 Family—ARAUCARIZ. 
 
 Genus—ARAUCARITES, Sternberg. 
 (Flora der Vorwelt, ii., p. 203.) 
 
 - ARAUCARITES P PotYcaRPA, Zen. Woods, PI. 18, fig. 1. 
 
 Araucarites ? polycarpa, Ten. Woods, Proc. Linn. Soc. N. 8S. Wales, 1883, viii., Pt. 1, p. 165. 
 oe australis, Ten. Woods, Ibid., t. 10, f. 1. 
 
 Obs. The late Mr. Woods did not give a description of this cone, but the few 
 characters now offered are taken from our specimen—which, although much smaller, may 
 possibly be the above species. The cone was probably elongate, and perhaps cylindrical ; 
 the scales are rhomboidal, with a subapical mucro, or stout blunt spine, but do not appear 
 to be ridged in the true sense of the word, nor divided into an upper or lower portion; 
 in each oblique row on the side visible there are about ten scales. 
 
 Now, irrespective of the size of the cone, there are obviously a less number of 
 scales in each spiral series in this specimen (PI. 18, fig. 1) than am Woods’ figure of 
 A.? polycarpa, and I think it questionable if the two can remain under the same 
 name, an opinion in which I am sustained by that of Mr. R. Kidston. In passing, a 
 reference might be made to those plant-remains from the South Australian Mesozoie 
 rocks, named by Dr. H. Woodward Mantellia babbagensis,* which bear a general 
 resemblance to our fossil. In addition to this cone, my Colleague has lately communicated 
 to me an almost complete impression, too late to be figured, of one four inches long 
 with a diameter rather exceeding three-quarters of an inch. It is a hollow external 
 cast contained in an ironstone nodule rather similar to Mr. Woods’ example. The 
 diameter of the present specimen is less than the latter, but the length is greater. 
 
 * Geol. Mag., 1885, ii., p. 290, t. 7, ff. 1 and 2. 3 
 
384 
 
 The scars were approximately rather smaller, and about the size of those in the figure 
 now given. So far as the specimen is preserved, thirty leaf-scales are visible in an 
 oblique row, and probably as many more would be so were the fossil complete. 
 Woods’ cast is much broader at the base, and less cylindrical than that just described. 
 The leaf-scales are two millimetres in vertical diameter, and about the same in the 
 contrary direction. 
 
 Loc. Stewart’s Creek, near Rockhampton (R. L. Jack). 
 
 Family—TAXODIACEZ. 
 Genus—SEQUOTLIITES, Carruthers. 
 
 SEQUOIITES ? AUSTRALIS, Zen. Woods. 
 Sequotites australis, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1888, viii., Pt. 1, p. 162, t. 7, f. 5. 
 
 Sp. Char. Leaves very close, two-rowed (?), spread out, flat, alternate, rarely 
 faleate, smooth above; midrib prominent below, rounded at the apex, towards which 
 there is only a very slight tapering, not contracted at the base but becoming a sheath, 
 down the centre of which the midrib can be distinctly traced, from twenty to twenty 
 five millimetres long, and one and a-half wide, but much shorter and smaller near the 
 extremities of the shoots, where they are somewhat imbricated all round the branch, 
 and loosely spiral; the sheathing base of the leaves gives rise to a jointed appearance to 
 the stem. (Ten. Woods.) 
 
 Obs. The Author justly speaks very cautiously of his reference of this plant, 
 only known from foliage, to Sequodites, “as no cones, either male or female, have 
 been hitherto discovered.” He adds—‘ We have no Australian conifer with leaves 
 similar to Sequoia except Podocarpus, but though in some species of that genus the 
 foliage is long, flat, and with a prominent midrib, there is a distinct petiole, which in 
 this fossil is wanting.” 
 
 Loc. Rosewood, near Rockhampton (The late Rev J. HE. T. Woods—Macleay 
 Museum, University of Sydney). 
 
 Family—TAXACEA, 
 
 Genus—TAXITES, Brongniart, 1828. 
 (Prod. Hist. Vég. Foss., p. 108. 
 
 TaxrTes MEDIus, Zen. Woods. 
 Taxites medius, Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. 1, p. 160, t. 9, f. 3. 
 
 Sp. Char. Branchlets thin ; leaflets spirally and bilaterally disposed, emerging 
 at an acute angle, sub-alternate, sometimes slightly curved outwards, narrow, linear, 
 obtuse, rather long; the decurrent pedicel thick, Jong, and broad (nearly as broad as 
 the leaf at times), midrib thick and conspicuous, surface shining and transversely wrinkled. 
 (Len. Woods.) 
 
 Obs. This is intermediate in character between the two Indian species 7. 
 tenerrimus, Feist., and T. planus, Feist. In the first of these the leaflets are very small 
 and horizontal, but in the second the leaflets are much broader and longer, although 
 horizontal also. 
 
 Loc. Ipswich (The Rev. J. FE. T. Woods—Macleay Museum, University of 
 Sydney). 
 
385 
 
 Genus—BRACHYPHYLLUM, Brongniart, 1828. 
 (Prod. Hist. Vég. Foss., p. 109.) 
 
 BRACHYPHYLLUM cRrassuM, Ten. Woods, Pl. 18, fig. 2. 
 
 Brachyphyllum crassum (aut. var. B. mamilare ?) Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, vii., 
 Pt. 4, p. 660. 
 “5 australe, var. crassum, Ten. Woods, Loc. cit., 1883, viii., Pt. 1, p, 159, t. 5. 
 
 Sp. Char. Plant robust, thick; stem and branches repeatedly dichotomous ; 
 leaves thick and fleshy, densely crowded, homodromous, short, broad, obtuse, conspicu- 
 ously keeled, erect, closely imbricate, but slightly spreading ; branches and branchlets 
 very little narrower than the parent stem, and of equal width to the summit; all 
 portions of the plant curved, three leaves visible in each spiral, and about three rows in 
 one centimetre. Length of leaves, from two to three millimetres; breadth, from five 
 to six; diameter of cauline stem at widest part, ten millimetres; of branchlets, eight 
 millimetres ; length of shortest, eighteen millimetres. (Ten. Woods.) 
 
 Obs. This is a very interesting plant, as the leaf-scars resemble those of 
 Lepidodendron. 
 
 Mr. Woods seems to have been in much doubt as to the name his fossil should 
 bear. At p. 54 of the Memoir cited*, in the list of Queensland Jurassic plants, he 
 mentions Brachyphyllum mamillare, but on p. 62 he gives B. mamillare, var. crassum, 
 whilst to the description on p. 159 is appended the name JB. australe, var. crassum. 
 By what name, therefore, is this plant to be known? With the view of avoiding this 
 confusion I have adopted his varietai name as the specific one, particularly as I believe 
 the plant in question to be distinct from Feistmantel’s species. This will also avoid any 
 confusion with Mamillaria Desnoyersii, which appears to have been dragged in without 
 any special object. If Mr. Woods intended to convey the idea that his B. crassum is 
 identical with the latter, why did he not adopt it as the specific name for the Queensland 
 plantat once? From the respective descriptions and figures of Feistmantel and Woods, it 
 seems to me that their species are distinct. In B. australe the leaves are said to be 
 flattened and sub-keeled; in B. crasswm they are described as conspicuously keeled. 
 These points are borne out by the Author’s figures. In fact, the short, broad, and 
 obtuse leaves on the branchlets of B. crassum correspond much more closely with the 
 somewhat similar leaves on the amentum of B. australe than they do with the rhomboid 
 oblong leaves on the branchlets of the latter. 
 
 B. crassum is said by its describer to closely resemble the European B. mami- 
 lare, Brong., but to differ from the latter, and all other known forms, in the 
 thickness and shape of the leaves, and the continuous branching without diminution of 
 diameter. The leaves are covered with a fine granulation, and have slightly raised 
 margins. Mr. Woods adds that the sharp and raised keel is not visible on all leaves. 
 A specimen before me, from Clifton Colliery, has some of the leaves keeled, others 
 not, but all with a more or less thickened margin. 
 
 On examining the figured type I find the characters laid down by Mr. Woods as 
 quite correct, and it is clear that where the vertical ridges have disappeared the plant 
 has been subjected to much pressure. The main branch of this specimen is six inches 
 long, and eleven millimetres wide, whilst the scales are from three to five millimetres in 
 transverse measurement. When really well preserved the leaf-scales have the form of our 
 Pl. 18, fig. 8, terminating upwards in a short mucro. This makes me hesitate the less in 
 referring this specimen also to B. crassum. In the example from the Walloon Mine, 
 
 * Author’s separate copy. 
 
 2A 
 
386 
 
 on the contrary, no edges or mucro are preserved, nevertheless it corresponds perfectly 
 with those portions of Woods’ type which are crushed. There is a very close 
 resemnblance between B. crassum and B. Papareli, Saporta.* 
 
 Loc. Tivoli Mine, Ipswich (The late Rev J. EB. T. Woods—Macleay Museum, 
 University of Sydney); Clifton Colliery, Ipswich (R. LZ. Jack); Rosewood, near 
 Ipswich, in ash-beds (Hon. A. C. Gregory). 
 
 Genus—CUNNINGHAMITES, Sternberg. 
 (Flora der Vorwelt, ii., p. 203.) 
 
 CUNNINGHAMITES AUSTRALIS, Zen. Woods. 
 Cunninghamites australis, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., Pt. 1, p. 165, t. 3, f. 1-3, 
 $14 feel, 
 
 Sp. Char. eaves long, linear, pointed, decurrent, entire ; male amenta in rather 
 thick corrugated clusters at the ends of the branches, generally two are alone distinct 
 in the fossil, but others can always be traced in the centre; amenta curved. (Ten. 
 Woods.) 
 
 Obs. The indistinetness of the figures quoted renders it impossible to follow 
 the specific characters laid down by Mr. Woods. He remarks that the presence of the 
 male amenta renders “ the identification of the genus much more certain. The leaves, 
 however, are seldom entire, which gives the appearance of an obtuse or unequal 
 foliage.” 
 
 Loc. Rosewood, near Ipswich (The late Rev. J. LH. T. Woods—Macleay Museum, 
 University of Sydney). 
 
 PLANTA INCERTA SEDIS. 
 
 Genus—CARDIOCARPUM, Brongniart, 1828. 
 (Prod. Hist. Vég. Foss., p. 87.) 
 
 CARDIOCARPUM ? AUSTRALE, Carruthers. 
 
 Cardiocarpum australe, Carruthers, Quart. Journ. Geol. Soc., 1872, xxviii., p. 356, t. 27, f. 4. 
 ? wustrale, Feistmantel, Palaeontographica, 1878, Suppl. Bd. iii., Lief, 3, Heft 3, p. 112. 
 
 Sp. Char. Fruit cordate, with an acute apex, and a ridge running along one 
 side of the fruit within and parallel to the edge; seed ornate, acute. (Carruthers.) 
 Loc. Tivoli Coal Mine, Ipswich (Lhe late R. Daintree). 
 
 Genus —CYCADINOCARP US, Schimper. 
 (Traité Pal. Vég., ii., p. 208.) 
 
 Obs. A name proposed for the seeds of Cycadaceous plants. They are 
 sub-globose, ovate, or oblong fruits, usually associated with stems and leaves of plants of 
 that order. In PI. 16, fig. 10, such a seed is represented, and resembles very closely 
 Cycadinocarpus rajmahalensis, Feistmantel.t 
 
 Loc. Wycarbah, near Rockhampton (The late James Smith). 
 
 
 
 * Pal. Franc. Terr. Jur. Vég., iii., t. 33. 
 + Pal, Indica (Gondwana Flora), 1877, i,, Pt, 2, p. 132 (80), . 35, f. 10, 
 
387 
 Kingdom—ANIMALIA. 
 Sub-King¢dom—A RTH ROPODA. 
 Class—CRUSTACEA. 
 
 Order—PHYLLOPODA. 
 Family—LIMNADIDZ. 
 
 Genus—ESTHERTA, Riippell and Straus, 1837. 
 (Mus. Senckenberg, 1887, ii., p. 119.*) 
 
 
 
 EsTHERIA MANGALIENSIS, Jones. 
 Estheria mangaliensis, Jones, Mon. Foss, Estherie, 1862, p. 78, t. 2, f. 16-28. 
 
 Sp. Char. Valves broadly subovate, hardly convex; dorsal margin straight, 
 about half the length of the valves, terminated at the anterior end by the umbones ; 
 anterior, posterior, and ventral margins fully and broadly rounded, the anterior shorter 
 than the posterior, rendering the valves narrower at the former of the two ends; 
 umbones depressed; ridges twelve in number, but probably two or three more exist on 
 each umbo, strong and well marked; interspaces wide, depressed, or perhaps very 
 slightly concave, especially towards the ventral portion of the valves; reticulation not 
 preserved. Length, about three-sixteenths of an inch. 
 
 Obs. This little fossil, the first /stheria found in the Secondary rocks of Queens- 
 land, appertains to the group represented by such species as EH. mangaliensis, LE. 
 Forbesi, &c., and, in fact is so very close to the former in its general features, that I feel 
 constrained to consider it as identical, notwithstanding the absence of the reticulated 
 surface in our fossil. It is particularly like Prof. Jones’ Pl. 2, fig. 16. 
 
 The Indian specimens are from the Mangali Beds of the Damuda Series, and the 
 occurrence of the species in the Ipswich Beds is but another link in the chain of 
 evidence uniting the great Secondary Coal-bearing Series of India with those of 
 Australia. 
 
 The specimen was obtained, with a magnificent collection of Mesozoic plants, by 
 Mr. J. H. Simmonds from the Ipswich Beds. 
 
 Loc. Denmark Hill, Ipswich Coal Field (J. H. Simmonds—Colln. Simmonds, 
 Brisbane). 
 
 Class—INSECTA. 
 
 Order—COLEOPTERA., 
 Family—BUPRESTIDZ. 
 
 Genus—MESOSTIGMODERA, Etheridge fil. and Olliff, 1890. 
 (Mem. Geol. Survey N. S. Wales, Pal, No. 7, p. 9.) 
 
 MesostiaMopERA Typica, EZ. and O. 
 Mesostigmodera typica, Etheridge fil. and Olliff, Mem. Geol. Survey N. S. Wales, Pal. No. 7, 1890, 
 Dod teiles teul-o. 
 Obs. A detailed description of this interesting Insect-Wing will be found atthe 
 reference quoted above, supplemented by the following remarks :— 
 “The remarkable character of the ornamentation or sculpture of this wing will 
 at once distinguish it from the various genera of the family Buprestide, both recent 
 
 
 
 * Fide T, R. Jones, Mon. Foss, Estheriz, 1862, p. 10. 
 
388 
 
 and fossil, and from the allied families Elateride and Eucnemide; indeed we cannot 
 recall, at this moment, a single genus throughout the whole Coleopterous order in which 
 the ordinary punctate-striate sculpture—consisting of distinct punctures arranged in 
 regular series one behind another—is combined with small irregularly disposed 
 elevations. Its form and structure clearly indicate that it belongs to the Buprestidae, 
 and there is little doubt, we think, of its affinity to that type of the recent genus 
 Stigmodera (e.g., S. gratiosa, Chey., S. Roe’, Hope, &c.), which prevails in Western and 
 South Australia. Thetypeof which wespeakis represented in New South Wales by one or 
 two species, and it is to one of these, 8. sanguinosa, Hope, that the fossil wing appears 
 to be most nearly ailied. The peculiar punctuation appears to indicate that this Insect 
 belongs to avery ancient type, and an examination of the specimen suggests the 
 possibility that the ordinary rugose form of sculpture, accompanied by deep pits, now 
 so prevalent amongst the Buprestide, may, so far as the Australian species are con- 
 cerned, have been derived from this older type.” 
 
 We are indebted to the researches of Mr. J. H.Simmonds for this very interesting 
 fossil. Other Insect remains were found by him at Ipswich, with one exception the 
 remains of Coleoptera. Two well preserved elytra are certainly referable to the 
 Rhynchophora, and one is evidently related to the genus Glochinorrhinus, or its 
 immediate allies. Two other fossils, exhibiting the thorax and elytra, are probably 
 representatives of the family Hydrophilaw, both of them having the wing-cases 
 punctate-striate, &c. A fifth specimen appears to be the head and pro-thoracie segment 
 of a Coleopterous larva, possibly of one of the Lampyrida, but in the absence of further 
 material, it is not judicious to venture a decided opinion. The only other specimen 
 which has, so far, been found, appears to be the impression of the abdomen of one of 
 the large Hemiptera. 
 
 Loc. Denmark Hill, Ipswich Coal Field (J. H. Simmonds—Colln. Simmonds, 
 
 mii. Sub-Kingdom—MOLLUSCA. 
 Section—MOLLUSCA VERA. 
 CLASS—PELECYPODA. 
 Order—UNIONACE. 
 Family—U NIONID. 
 
 Genus—UNIO, Phillipson, 1788. 
 (Dissert. Hist. Nat. Nov. Test. Genera, p. 16.) 
 
 UNIO IPSVICIENSIS, sp. nov., Pl. 42, figs. 2 and 3. 
 
 Sp. Char. Transversely elongated, narrow, wedge-like, sub-acute posteriorly. 
 Dorsal or cardinal margin short, much less than the length of the shell; ventral margin 
 generally rounded, but straight towards the centre. Anterior end short and rounded ; 
 posterior end produced and obtusely pointed Umbones small, quite anterior, and 
 much eroded. No true posterior slope, but the flanks insensibly graduating into the 
 posterior end. Surface with concentric roughened corrugations. 
 
 Obs. This species is so generally like many other species of Unio that it is 
 difficult to point out its distinctive characters. It is a very much smaller species than 
 the following one, and it is quite distinct from anything yet described from Australian 
 Mesozoic rocks. 
 
 Loc. Shaft at the Bremer Basin Colliery, at a depth of two hundred feet 
 (H. Heaviside). 
 
389 
 
 fa’ Unio Eynrensis, Tate. 
 Unio Eyrensis, Tate (m.s.) 
 
 »” Etheridge fil., in H. Y. L. Brown’s Reports on Coal-bearing Area in the Neighbourhood of 
 Leigh’s Creek, S. Austr. (S. Austr. Parl. Papers, 1891), p. 11, t. 2, f. 1-3. 
 
 Sp. Char. Shell transversely elongate, or elongately subovate, length more than 
 twice the height; anterior end slightly produced, posterior end obtusely pointed, 
 and produced ; hinge-line behind the umbones obliquely inclined; ligamental area 
 broad; ventral margin convex; umbones tumid, depressed, and much eroded; 
 anterior muscular impressions low down, the posterior small and close under the 
 hinge-line ; shell moderately thick, surface representing the epidermis coarsely striate 
 and subimbricate. 
 
 Obs. This species is represented by two examples, one an internal cast with 
 portions of the shell still remaining, the other a more complete individual, with nearly 
 the whole of the shell preserved and the umbones eroded. The specimens are con- 
 verted into ironstone, and their appearance is so different from the other North Queens- 
 land fossils as to at once suggest a totally different deposit. 
 
 The species of Unio hitherto deseribed from Australian rocks are very limited in 
 number, and we have now in consequence to deal with one of an entirely new facies. 
 U. eyrensis resembles to some extent the species from the Judith River Group 
 of North America, but is a more convex and bulky form, and devoid of radiating 
 strie. 
 
 Unio Dane, Meek and Hayden,* from the Laramie Group (Cretaceo-Tertiary) , 
 resembles the present Species to some extent, but is not so nasiform, or elongately 
 wedge-shaped. 
 
 Amongst European Wealden species it is not unlike J. porrectus, Sby., but still 
 more like Unio sub-porrectus, A. Roemer,+ or U. Dunkeri, Struckmann.t 
 
 Loc. Bundanba, near Ipswich, in brick clay overlying coal (Hon. A. C. Gregory, 
 and J. Malbon Thompson). 
 
 Unto, sp. ind. 
 
 Obs. A second species occurs in the same bed at the Bremer Colliery, but it is 
 distinct from U. ¢psviciensis. It is far larger than the latter, and evidently differed 
 much in shape, being a broader and stronger species. The specimen consists of the 
 anterior portion of the conjoined valves, and had Jost all trace of shelly matter. It is 
 too imperfect for further diagnosis. 
 
 E. 
 
 Se 
 * White in Powell’s 8rd Ann. Report U. S. Geol. Survey, 1881-82 [188 t. 17, f. 1-3 
 + Dunker, Mon. Norddeutchen Wealdenbildung, 1846, p. 27, t. 11, f. 6. 
 ¢ Die Wealden-Bildungen, 1880, t. 1, f. 6. 
 
CHAPTER XXXI. 
 
 THE ROLLING DOWNS FORMATION (LOWER CRETACEOUS). 
 
 ARTESIAN WELLS. 
 
 As will be seen by the Geological Map, the “Rolling Downs Formation’’ covers 
 an area which may be roughly stated at three-fourths of the total extent of the Colony. 
 It extends westwards from the Paleozoic ranges on the east coast, from near the heads 
 of the Macintyre in the south to the Palmer in the north. West of this line it occupies 
 the whole of the Colony, save where it is unconformably overlaid by the Desert 
 Sandstone, and where the Paleozoic rocks of the Cloncurry, and of De Little, Cairn, 
 and the Grey Ranges rise from beneath it like islands. Westward and southward it 
 extends across South Australia into Western Australia and New South Wales. Except 
 in Queensland, however, it appears to be covered to a considerable extent by Tertiary 
 rocks. It marks the position of a sea which in Cretaceous times divided the Australian 
 Continent into two islands. 
 
 The Ipswich Coal Field seems to pass upward into the Rolling Downs Formation, 
 although the junction has not yet been satisfactorily traced. To draw a definite line 
 between the Ipswich and the Rolling Downs Formations is quite impracticable, but the 
 appearance of Belemnites and Ammonites, with other marine forms, in the latter, suff- 
 ciently marks the change from the plant-bearing beds of the former. 
 
 Everywhere in the North the Rolling Downs Formation lies directly, and of 
 course unconformably, on schists and slates of undetermined age, or on granite or 
 gneiss, the Ipswich Formation being unrepresented. The “ Rolling Downs” is by nomeans 
 a mountain-forming formation. Generally, its decomposition forms a rich soil which is 
 taken possession of by the nutritious “ Mitchell’? and “ Blue’ grasses, so highly favour- 
 able totherearing of sheep and cattle. The surface rises into a series of gentle undulations, 
 not, however, of sufficient importance to disturb the idea of a dead level. Travelling 
 over the “ Downs” becomes monotonous after a few days, the sun rising in the east and 
 setting in the west on the horizon of an ocean-like plain. The watercourses which intersect 
 it are dry for the greater part of the year, except for a few waterholes, and are so ill- 
 defined that it is hard to tell in dry weather which way the water flows in wet. 
 Each watercourse is marked by a straggling fringe of timber, while the rest of the plains 
 are treeless. As the streams are of this character, it results naturally that they » 
 rarely cut through the soil, and consequently sections of the strata occur only at wide 
 intervals. 
 
 The monotony of the scenery is the direct result of a sameness of composition 
 throughout the whole series. 
 
 In announcing the discovery, in 1867, of a suite of fossils by Mr. W. P. Gordon, in 
 Wollumbilla Creek,* the late Rev. W. B. Clarke ¢ referred to the “ pale sandstones of 
 the creek, and hard red conglomerates and quartzites from between Wollumbilla and the 
 River Amby.” [The latter probably Desert Sandstone.] Subsequently Mr. Clarke f{ 
 stated that the Wollumbilla fossils occurred in rounded, nodular, or concretionary 
 boulders, imbedded in a brittle marl in the creeks, and on the downs, which are covered 
 
 
 
 * Wollumbilla Creek is crossed by the Western Railway, 294 miles from Brisbane. 
 + Quart. Journ. Geol. Soc., xviii. (1862), p. 245. 
 + Recent Discoveries in Australia, :p. 52. 
 
391 
 
 by grits and sandstones, mostly red and evidently partly fused by igneous action 
 [Desert Sandstone]. The calcareous sandstone occurs along the creeks and downs 
 where water has denuded it ; and, above all, is a coarse grit. The descending section 
 
 in the creek bank, where the fossiliferous nodules occur, at Wollumbilla, is as 
 follows :— 
 
 1. Brown stiff clay, full of pebbles of quartz, much waterworn. 
 
 2. Clay. 
 
 3. Slate-coloured marl, very friable above, but hard below, charged with strings 
 of crystalline carbonate of lime, and breaking into rectangular fragments. 
 In this oceur the calcareous masses. The height of the section is about 
 fifteen feet. On the east, at about three miles distance, coarse con- 
 glomerates rise above these beds. The bluff end of the conglomerate rises 
 to about twenty feet. [The conglomerates referred to after the words in 
 italics must be the Desert Sandstone. | 
 
 “The caleareous boulders from the Wollumbilla Creek, when broken, are found 
 to be of a deep olive colour internally, a few presenting a dull brown or bluish hue 
 They are very compact. In all of them organic remains are very abundant. The 
 exteriors of many of the boulders are much waterworn, and exhibit only sections of the 
 organic remains they contain, whilst in others a certain amount of decomposition or 
 oxidation of the surface has taken. place, which has produced a rotten exterior, looking 
 like an impure chalk, of a yellow or buff colour. Where this is the case the fossils 
 stand out sharply from the matrix.” 
 
 I may observe that I do not agree with the Author as to the waterworn condition 
 of the boulders, which are probably concretionary masses weathering spheroidally. 
 
 The Wollumbilla fossils were described and figured by Mr. Charles Moore, 
 F.G.8S., in 1869.* I do not propose to repeat Mr. Clarke’s or Mr. Moore’s lists, 
 which are incorporated, with annotations, in my Colleague’s observations. Mr. Moore’s 
 conclusion as to the age of the deposits is as follows :— 
 
 “Tt is not easy to decide with certainty as to the exact position of the fossils 
 that come from Wollumbilla. The Lias, the Great Oolite, the Oxford Clay, the 
 Portland Qolite, and the Cretaceous Beds may each put in a claim; but that of the 
 Oxford Clay appears to be strongest. That they all belong to the Upper Oolite may with 
 safety be inferred.’ Of the Bungeworgorai and Amby Beds, in the same neighbourhood, 
 Mr. Moore says, “From the nature of the matrix, though this does not pass for much, 
 they appear to have been derived from beds of a different character from those from the 
 other districts. As similar Criocerata have never been found below the Lower 
 Greensand, it is reasonable to infer the presence of Neocomian Beds in Australia, from 
 whence it may have been derived.” 
 
 Mr. Daintree mentioned in 1868 + the occurrence of Belemnites on the Dugald 
 River, Cloncurry District. 
 
 In accompanying Hann’s Northern Exploring Expedition in 1872, Mr. Norman 
 Taylor discovered richly fossiliferous deposits in the Walsh District. From notes which 
 he has kindly placed at my disposal, I make the following extracts :— 
 
 “At Camp 11 on the Walsh River, and likewise at Camp 79 (return 
 journey),{ at Elizabeth Creek [near what is now Wrotham Park Station], where mostly 
 
 
 
 * Quart. Journ. Geol. Soc., xxvi., p. 226. 
 
 + Report on the Cape River Diggings, and the latest Mineral Discoveries in Northern Queenslard 
 Brisbane: by Authority: 1868, 
 
 + The positions of the Camps referred to are laid down (Mr. Taylor says not very accurately) on the 
 map attached to Mr, Hann’s “ Diary of the Northern Expedition.” Brisbane: by Authority : 1873. 
 
392 
 
 Belemnites were found ina calcareous conglomerate. In a creck a short distance to the 
 north-east of Camp 81 (return journey), there occur large quantities of ironstone 
 nodules, in one of which I discovered a fine and very perfect crustacean, which, however, 
 appears to have been lost,* as it was not noticed by Mr. Etheridge, senr., when describing 
 the Collection. The Mesozoic rocks here rest on a grey felsitic quartz-porphyry. 
 
 “At Camp 11 the Mesozoic beds consist of thin-bedded brown, olive, and 
 whitish concretionary shales, passing downward into blue marly-shales, having a 
 crystalline efflorescence on the surface (sulphate of soda?) and decomposing rapidly. 
 The olive-coloured limestone concretions form lines (in the shales) in the cliffs, like 
 the flints in the chalk of England. These beds dip slightly northwards, and are faulted 
 in several places, and are jointed east and west. To the south the plains are occasionally 
 covered with these boulder-like concretions and glazed ironstone pebbles. 
 
 “At Elizabeth Creek, between Camps 11 and 18, the cliffs consist of red and white 
 conglomerates t passing downwards into sandy beds, which rest on blue shales and 
 gypseous marls, with thin layers of gypsum and cone-in-cone limestone. Septaria also 
 occur with veins of dolomite and centres of cale-spar. Irregular patches of red and 
 yellow concretionary ironstone also occur, some pebbles having an external jet-black 
 polish. With the exception of a fragment of an Orthoceras,§ the only fossils I could find 
 were Belemnites in a calcareous conglomerate at the base of the cliffs and obscured by 
 talus. 
 
 “At Camp 14, Mesozoic blue shales and concretionary limestones occupy the 
 river bed, overlaid by a grey jointed calcareous sandstone. The rounded flattened 
 concretions (not boulders) in these beds, as well as the beds themselves, contain a rich 
 store of fossils, especiaily Cephalopoda (Ammonites, Crioceras, &e.). These fossil 
 beds are everywhere overlaid by siliceous pebbly conglomerates, coarse grits and 
 sandstones, and ironstone and ferruginous grits.” || 
 
 “In a letter from the late Rev. W. B. Clarke to myself, dated 4th June, 1874, 
 he says: “ Prof. Etheridge (senr.) says of the Walsh River fossils, ‘there is no 
 specimen of Orthoceras in the entire series,’ and Mr. Carruthers writes thus: ‘ There 
 is not sufficient to warrant establishing a species, but the fragments point to a form of 
 Laeniopteris, nearly allied to Strangerites ensis (Oldham and Morris in Indian Survey 
 Memoirs), which Schimper calls Angiopteridium. We must have more materials, 
 however, before we can be certain.’ ”’ 
 
 The following is Mr. Etheridge’s description of the Walsh River fossils, quoted 
 in a letter of the late Mr. K. T. Staiger, the then Curator of the Queensland Museum, 
 Brisbane, dated 8th May, 1874. 
 
 “The Walsh River fossils consist of the following forms:— 
 
 CEPHALOPODA. 
 Ammonites, allied to A. clypeiformis. 
 Ammonites, sp. (?) | 
 Crioceras (4), sp. 
 
 All from nodules. 
 Belemnites (2), sp. | 
 
 
 
 * In a letter to me, dated 25th October, 1879, Mr. Taylor says : “ In looking over the list of Queensland 
 Exhibits, at Sydney, I find one by the Trustees of Brisbane Museum of a Crustacean unknown, from the 
 Walsh, which must be my missing specimen.” (R.Z.J.) The specimen exists in the Queensland Museum, 
 and will be described. (R. E. Junr.) 
 
 + Mr. Skene, of Wrotham Park Station, assures’ me that Ammonites and Belemnites occur at 
 Elizabeth Creek in situ. (R.L.J.) 
 
 + Desert Sandstone, apparently. (R.Z..J.) 
 
 § Probably the phragmacone of a Belemnite. (R. Z. junr.) 
 
 || Desert Sandstone? (R,L.J.) 
 
393 
 
 BIvVALVE SHELLS. 
 
 Myacites Hinnites 
 
 Byssoarca Cytherea 
 
 Solemya Cyprina 
 
 Arca Myoconcha . 
 Panopea Pecten 
 
 Inoceramus Teredo in fossil wood. 
 
 ‘‘T believe the whole of these are Cretaceous (Lower) and one perhaps Neocomian. 
 Most of the species are new, but to figure and describe them would serve no good pur- 
 pose, as they are all apparently in drift nodules, and can hardly have been found in situ. 
 I shall always have much pleasure in rendering you what assistance I can in these 
 matters, but I would at the same time point out the uselessness of sending home any 
 fossils for determination which are simply drifted surface specimens. The perplexing 
 mixture of forms from Wollumbilla, previously described by Moore, arose from this 
 collection of specimens from drifted nodules. The whole series will be returned to the 
 Colony as soon as Mr. Carruthers has completed his investigation of the supposed speci- 
 mens of Glossopteris.”’ 
 
 Mr. Taylor continues:—‘‘ No mention is made of some fine Ichthyosaurus 
 vertebrex discovered on the Walsh by Warner (one of our party), or of my Crustacean. 
 
 “The Mitchell River bed is composed (at Camp 14) of thin grey shales and brittle, 
 conchoidally fractured, marly mudstones, full of large and small flattened globular 
 concretions. The mudstones are full of Dentaliwm (?) and small bivalves (Leda 7), 
 and the concretions of large bivalves and Cephalopoda (Pecten, Ammonites, &c.) always 
 lying on their flat surfaces. That they have been formed cn situ by segregation of the 
 calcareous matter round the decomposing animal, there can be no doubt. The idea of 
 their drift origin is simply preposterous.” 
 
 Caicareous nodules, such as are described by Mr. Taylor, are of common occur- 
 rence among the shale beds all over the Rolling Downs, and I have no doubt that Mr. 
 Taylor’s fossils were found zz situ. At the same time the misconception on the part of Mr. 
 Etheridge probably arose from the imperfect data concerning the occurrence of the 
 fossils with which he was furnished. As a matter of fact, am given to understand that 
 the Ichthyosaurus vertebre, from what cause I cannot tell, never reached Mr. Etheridge. 
 
 The late Mr. R. Daintree remarked * that “all the great plains of Queensland 
 westward of the Main Range consist of subaérially decomposed Oolitic and Cretaceous 
 shales, limestones, and sandstones ;” and, further—“ The only variety in the lithological 
 character of the Flinders and Thompson Rivers Mesozoic rocks is the change from 
 shale to fine-grained sandstone in the alternating beds, the shale greatly predominating , 
 its line of bedding marked by thin bands and nodular layers of argillaceous limestone.” 
 
 “One other peculiarity in the strata forming the series is the presence at intervals 
 of thin layers of limestone having the well-known cone-in-cone structure. This has 
 more the appearance of a chemical precipitate than a.mechanical deposit, and contains 
 no fossils. Its analysis gave :— 
 
 
 
 Insoluble in hydrochloric acid .., es <6 cee a .. 14°920 
 Ammonia-precipitate ... eae 7A ae ses vas .» 4860 
 Carbonate of lime or Fis aa +4 ase = .. =75'458 
 Undetermined constituents... A ive — es ww» «=—«4762 
 100°000 ” 
 
 * Quart. Journ. Geol. Soc, 1872, xxviil., p. 282, 
 
394 
 
 Speaking of the collection examined by Mr. Moore, Daintree suggests * that “ it 
 is possible that fossils from different localities, or perhaps drift specimens, have been 
 mixed up.” 
 
 In the same Paper Mr. Daintree (p. 278) remarked that “a single shell (Tellina) 
 found in a bed of horizontal limestone at the head of the Gregory on the Barkly Tableland, 
 and forwarded to me by the Rev. W. B. Clarke, of Sydney, would, if belonging to this 
 Desert Sandstone [Series], as it probably does, give reason to believe that the lacustrine 
 condition may be eliminated.’ This observation is noticed merely for the purpose of 
 correcting Daintree’s mistake, the limestone of the Barkly Tableland having since 
 proved to belong to the Rolling Downs Formation. 
 
 Daintree continues as follows:—‘ As early as 1866, a suite of fossils was 
 collected by Messrs. Sutherland and Carson (of Marathon Station) on the Flinders 
 River, and forwarded for determination to Prof. McCoy in Melbourne. They were 
 never figured +; but his manuscript names are as follows ft :— 
 
 REpTILIA. 
 Ichthyosaurus australis, McCoy. 
 Plesiosaurus Sutherlandi, McCoy. 
 Plesiosaurus macrospondylus, McCoy. 
 
 CEPHALOPODA. 
 Ammonites Sutherlandi, McCoy. 
 A. Flindersi, McCoy. 
 Belemnitella diptycha, McCoy [=B. Canhami, Tate]. 
 Ancyloceras Flindersi, McCoy. 
 
 LAMELLIBRANCHIATA, 
 
 Inoceramus Carsoni, McCoy. 
 a Sutherlandi, McCoy. 
 
 “One locality being assigned to all the fossils alluded to in the above notice, it 
 was evident to me that either fossils from different localities had been mixed together, 
 or derived specimens had been mingled with those obtained in sétw, and no satisfactory 
 conclusion or inference could be drawn, for purposes of correlation with European, 
 Asiatic, or African forms. In company with Mr. Sutherland, who supplied McCoy 
 with the before-mentioned materials, I therefore visited the Upper Flinders and care- 
 fully collected the fossils from three localities—viz., Marathon Station, Hughenden 
 Station, and Hughenden Cattle Station. ; 
 
 “At Marathon, which is some forty miles further down the Flinders than 
 Hughenden, there is, close to the homestead, au outcrop of fine-grained yellow sand- 
 
 
 
 * Loc. cit. p. 282, 
 + Prof. (now Sir. F.) McCoy published his researches on these fossils in a series of Papers entitled as 
 follows :— 
 (1.) A Note on the Cretaceous Deposits of Australia, Ann. and Mag. Nat. Hist., 1865, 3rd Ser., xvr., 
 p. 332. 
 (2.) On the Discovery of Cretaceous Fossils in Australia. Z'rans. R. Soc. Vict., 1866, vii., pp. 49-51. 
 (3.) On the Occurrence of Jehthyosaurus and Plesiosaurus in Australia, Ann. and Mag. Nat. Hist., 
 1867, 37d Ser., xix., p. 355. 
 (4.) On the Discovery of Lnaliosauria and other Cretaceous Fossils in Australia. Z'rans. R. Soe. 
 Vict., 1868, viit., p. 41. 
 From these references, it will be seen that Sir F. McCoy was absolutely the first to announce the occurrence 
 of Cretaceous fossils in Australia. 
 + Without the attached notes, 
 
395 
 
 stone, which has been quarried for building purposes ; and below this, down to the edge 
 of a waterhole supplying the house, is a series of sandstones and argillaceous limestones, 
 containing numerous organic remains. 
 
 “These I have submitted to Mr. Etheridge [Senr.], for examination and correla- 
 tion, the result of which will appear in the Appendix to my paper; I, however, attach 
 here a summary of the forms determined by him from this locaiity :— 
 
 Inoceramus marathonensis, Eth.* 
 
 ‘, allied to problematicus. 
 £ pernoides, Eth. 
 s multiplicatus, Stol., var. elongatus, Eth. 
 
 “From these beds also came McCoy’s Reptilia. 
 
 “The ‘Marathon’ Beds, as they may be designated, are undulating, with an 
 uncertain dip. Proceeding from ‘ Marathon’ up the Flinders River (most probably over 
 a series of older beds) no cliff-sections are met with; but at Stewart’s wash-pool, on 
 the main road, the Avicula hughendenensis, Eth. [=Aucella hughendenensis, Eth. fil.] 
 of Hughenden is found in abundance. 
 
 “At Robert Grey’s Hughenden Station, however, which lies about three miles 
 east of Mount Walker, a series of calcareo-argillaceous beds crop out, containing a 
 marked and well-preserved fauna, indicating no great difference in facies from that of 
 Marathon.” 
 
 A section accompanying Daintree’s text “of a cliff on Bett’s Creek, intermediate 
 between Marathon and Hughenden,” and another “on the bank of the Flinders,” ‘‘ show 
 how nearly horizontal the great Mesozoic system of the Flinders remains; but the 
 latter indicates their general dip towards the north-east [north-west must be meant], 
 and therefore places the Hughenden Beds below those of Marathon. The observations 
 collected on the journey between these two places give the same result. The paleeonto- 
 logical evidence is not sufficient to enable Mr. Etheridge [Senr.] to draw any great line 
 of demarcation. His determination of the species from the Hughenden beds is as 
 follows :— 
 
 Ammonites Beudanti, D’Orb, var. Mitchellii, Eth. 
 5 Daintreei, Eth. 
 
 Avicula hughendenensis, Eth. 
 
 Pecten, &e. 
 
 ““These were obtained from horizontal calcareo-argillaceous beds, fronting the 
 water-hole where the sheep-wash is placed, about half a mile from the Hughenden 
 Station. The Avicula bed, which is a very marked band, about four inches thick, gives 
 by analysis :— 
 
 
 
 Residue insoluble in HCl, chiefly clay .. bas ey pr 8) 
 Ammonia-precipitate, of which 1°219 per one was fone oxide .. 9368 
 Carbonate of lime.. ka = rom or ie a .. 67°888 
 Carbonate of eeaean oes ot a wae 50 nae ree i020) 
 Undetermined, water, &c. abe tee ae ab; aus soo PAE! 
 100°000 
 
 “The Hughenden Cattle: station is twenty miles further up the Flinders than the 
 Hughenden Head Station. Here hundreds of Belemnites are strewn over the surface of 
 the two ridges which front the Cattle-station huts, but they are rarely found in the soft 
 shales which crop out from under an escarpment of‘ Desert Sandstone.’ 
 
 
 
 *The names quoted here must be understood to be subordinate to those hereafter given by my 
 Colleague. 
 
396 
 
 “The lithological character of these Cretaceous strata is such that decomposition 
 is rapid; and cliff-sections are accordingly very rare, the resulting physical aspect being 
 that of vast plains, which form the principal feature of Queensland scenery west of the 
 main dividing range ; but that the ‘ Desert Sandstone’ has extended over all this country 
 is evidenced by its existence either in the form of outliers or as a marked feature in situ 
 on all main watersheds, or by its pebbles of quartz and conglomerate, which are strewn 
 everywhere over the surface of the plains. 
 
 “The height of the watershed between the Thompson and the Flinders Rivers 
 is locally not more than 1,400 feet above sea-level; and as the former river has to 
 travel as many miles before reaching the sea, it is easy to understand why, in a 
 country subject to heavy tropical rains at one period of the year, followed by a long 
 dry season, the river channels are ill-defined, and vast tracts of country covered by 
 alluvial deposits.” 
 
 Mr. Robert Etheridge, F.R.S., in an Appendix to Mr. Daintree’s Paper, gave a 
 detailed description of the fossils from the Flinders area, which need not here be 
 repeated, as in the following pages the names and descriptions are recapitulated, 
 with annotations and the results of a fuller experience, by my Colleague. 
 
 Speaking of the material which formed the subject of Mr. Moore’s paper 
 already referred to, Mr. Etheridge says * :—“ It is, however, to be regretted that his 
 specimens were not obtained im situ, instead of from drifted materials; for nothing 
 is known of the beds or sections from which the Wollumbilla fossils originally 
 came. It is not a little singular, however, that Mr. Moore recognised twenty 
 species as common to England and Western Australia.” In this, and the same 
 Writer’s remarks on Mr. Taylor’s Walsh fossils, as well as in Mr. Daintree’s remarks, 
 we can trace the steady growth of the misconception which I believe was started by 
 the Rev. W. B. Clarke’s error in taking the Wollumbilla nodules for drifted boulders. 
 
 From the imperfect materials at his disposal, and taking his stratigraphical 
 information, it must be remembered, at second-hand, Mr. Etheridge read the sequence 
 of the Mesozoic and Cainozoic strata, as follows :— 
 
 Pleistocene. 
 Upper Volcanic. 
 Desert Sandstone. 
 Lower Volcanic. 
 ( Marathon Beds. 
 , | Cretaceous 4 Hughenden Beds. 
 Maryborough Beds. 
 
 Cainozoic 
 
 Teniopteris [Tivoli and Burrum Coal Measures]. 
 ¢ Oolitic } ele Beds. Lias and Oolite. 
 Gordon Downs Beds.t 
 
 I may say here that later stratigraphical observations show, and paleontological 
 research corroborates, that the Burrum Coal Field is older than the Ipswich (repre- 
 sented by Tivoli in the above list); that I regard the Hughenden, Marathon, and 
 Wollumbilla Beds as practically on the same horizon and of Lower Cretaceous age; 
 and that the Desert Sandstone and Maryborough Beds are identical and Upper 
 Cretaceous. 
 
 Sir Richard Owen describes { under the name of Wotochelys costata, Owen,§ a 
 Chelonian reptile from the Flinders River. 
 
 Mesozoic 
 SS Se 
 
 * L0¢. Cit., DP. o2os 
 
 + Gordon Downs, near Roma, the locality referred to, must not be confounded with Gordon Downs 
 at the head of the Roper, near Clermont, where Permo-Carboniferous Coal Measures occur, 
 
 + Quart. Journ. Geol. Soc., Vol. xxxviii., p. 178. 
 
 § Hereinafter described as Wotochclone costata, Owen, sp. (R. E. Junr.) 
 
4 
 
 397 
 
 The Rey. T. W. Ramm, in 1885, presented to the Geological Survey Collec- 
 tion, a Cephalopod from the Flinders River, near Hughenden, which I took 
 for Orthoceras, but which my Colleague now identifies with Belemnites Selheimi, 
 Ten. Woods. 
 
 The extracts above quoted appear to exhaust the stratigraphical and litho- 
 logical information recorded by former writers on the Rolling Downs Formation, and 
 I now add what I have myself observed in various traverses of the Western District. 
 
 From the junction of Julia Creek with the Cloncurry north-westward to Gregory 
 Downs, the strata of the Rolling Downs Formation can be traced. 
 
 At Kamilaroy, on the Leichhardt River, and the ‘ Grass Gunyah,” twelve miles 
 south-west of Kamilaroy, are extensive outcrops of magnesian limestone. At Kamilaroy 
 the limestone yielded specimens, among which my Colleague recognised Belemnites ; 
 Otodus apendiculatus, Agassiz; vertebre of a Teleostean fish; and a posterior costal 
 plate of a Chelonian. 
 
 On the Leichhardt, nine miles from the mouth of Gunpowder Creek, ancther 
 limestone yielded Belemnites, a portion of the tooth of Zamna, and Aucella hughen- 
 denensis, Eth. 
 
 Running up the Gregory River, Paleozoic rocks occupy the greater part of the 
 distance from Gregory Downs to the mouth of the O’Shanassy. Carl Creek Police 
 Station is situated on the right bank of Carl Creek, a fine rushing stream, which leaves 
 the Gregory and runs into the O’Shanassy. Behind the barracks is a large open plain 
 bounded on the south by cliffs of a hard yellow limestone, horizontally bedded. 
 This limestone evidently occupies an ancient depression, and overlies (unconformably) 
 nearly vertical Paleozoic sandstones, &c. Thesummit of this limestone forms a plateau 
 which extends to Rocklands under the name of Barkly’s Table-land. The occurrence 
 of Tellina on Barkly’s Table-land has already been noted. 
 
 On the Upper Flinders, eighteen miles N. 29° W. of Coalbrook Railway 
 Station, on the Northern Railway, the Rolling Downs Formation is seen beneath the Desert 
 Sandstone. The uppermost beds seen are soft crumbling dark-grey shales, about sixty 
 feet in thickness, with bands of red ferruginous sandstone or arenaceous ironstone and 
 grey limestone. Thence, down to the level of the river, are seen about ten feet of dark, 
 fine-grained, felspathic sandstone. The surfaces of the sandstone beds in the river are 
 in places covered with obscure markings suggestive of the tracks of gigantic reptiles. 
 The beds of the Rolling Downs Formation seen in this section, although nearly hori- 
 zontal, undulate slightly, but their general tendency is to dip down the river, while the 
 Desert Sandstone remains horizontal, thus affording a new instance of the unconform- 
 ability observed elsewhere between the two formations. The shaly beds of the inferior 
 formation, with their bands of ironstone and limestone, bear a close resemblance to the 
 portion of the Rolling Downs Formation exposed in the neighbourhood of Hughenden. 
 A few hundred yards up the river, the rise of the strata exposes beds on a lower horizon 
 than those above described. These are thick-bedded sandstones, partly of felspathic 
 but mainly of siliceous materials, varying into grits, pebbly grits, and conglomerates. 
 About two miles further up the river the following section is seen on the left 
 bank :-— 
 
 Section No. 1. 
 
 Ft. in. 
 (a) White gritty and pebbly sandstone aa oe a ae eae O 
 (6) Laminated grey micaceous clay... fc ah or Hs we O49 
 (eye Coal. © 3: Re a me sh - i Ha ae »» O25 
 (d) Fine-grained brown siliceous shales, with plant-remains or Moye At 
 
398 
 
 ee 
 
 DAOOWNHOAE 
 
 Coal soe dee G 8 ies oh oo “nc 
 (e) | Broa laminated clay = a 5c ae “is et Dio 
 Coal ss 
 Black mud with coaly str eaks 
 
 Grey-brown shale, with coaly specks and streaks 
 
 (f) 
 Coal . ory foe as cas 
 Grey shales with ehaly streaks a 5 
 
 (9) Coal in bed of river (bottom of seam not nie 
 
 On the right bank of the river, about one chain below the last section (south- 
 south-west), the following section was measured :— 
 
 bole 
 
 HOrFOOOOF 
 
 S 
 Oo 
 
 Section No. 2 
 
 Ft. in. 
 (a) Sandstone ae 40 0 
 (6) Laminated grey micaceous clay or le ve US 
 (c) Coal ee 0 2 
 (dq) Fine-grained brown wliceous alihs with plantar remains 0. 25 
 (e) Coal ae * ik As 
 (f) Dark-grey shale or fire- clay, with “Abin remains se eer 
 (g) Coal in bed of river (bottom not seen) 0 7 
 
 On the left bank of the river, about three chains above Section No. 1, the 
 following section was seen :— 
 
 Section No. 3. 
 
 Ft. in. 
 Coal bes Leal 
 (a) | aris sandstone fed 0 13 
 Coal 0 2 
 Brown hard unlaminated siliceous clay, with coaly streaks, i in hibed of 
 river (bottom not seen) .. a) iy; sf re ee +, 6 Das 
 
 In the above three des the identifiable beds are distinguished by italic 
 letters. 
 
 An analysis of a sample of seam (9g) gave the following results :— 
 
 Water ae Be red nae a2 He ae im 8°30 
 Volatile hy drocasbane “pa a ae ‘al ie ai ay. SYfae 
 Fixed carbon dee are we a ae ho be oe LO LOs 
 Ash oe eee nee va as ase Bae “eke sae 2°80 
 
 100:00 
 
 Specific gravity 1°38. 
 
 The coal scarcely soils the fingers, and gives a jet-black powder. The ash is 
 white, with a faint yellow tinge, and mainly siliceous. The coke is hard and firm. The 
 small amount of incombustible residue, and the proportions of volatile hydrocarbons, 
 and fixed carbon, make this coal a very valuable one, either for gas-making or steaming 
 purposes; in fact, it may be pronounced to be a better coal than some of the most 
 highly prized coals of Newcastie (N.S.W.). The thickness of the overlying Desert 
 Sandstone is not great, and may place no very serious difficulty in tracing the coal-seams, 
 should any be found of workable thickness, to the railway line.* 
 
 In the Diagram (PI. 45, fig. 1) the relation of the Rolling Downs Formation to the 
 granite and other rocks, as seen at Tatoo Camp, in a gully near the head of the 
 
 
 
 
 
 * Report.by R.L.J. on Coal Discoveries on the Flinders. Brisbane: by Authority : 1888, 
 
399 
 
 Flinders, is well shown. It rests on the granite, and is overlaid unconformably by the 
 Desert Sandstone, which overlaps it, and abuts against the granite. The Desert 
 Sandstone itself is covered by lava-form basalt beds which overlap it and appear again in 
 great force on the Burdekin side of the granite range. The altitude of Tatoo Camp 
 was estimated (by Aneroid) at 1,840 feet. 
 
 On the Dalrymple Road, twelve miles above Hughenden, a guliy, risingin Mount 
 Beckford, and falling into Porcupine Creek, exposes a section of about twelve feet ef 
 horizontally bedded grey clay shales, with thin bands of grey flags and “ damper-shaped ” 
 nodules of magnesian limestone, each enclosed in an envelope of glittering carbonate of 
 lime. Exactly similar strata are exposed at Hughenden Township, in the Chinaman’s 
 Gully, and at the washpool from which Daintree obtained some of his fossils. I could 
 see, however, only a few Belemnites, and some shells, all in bad preservation. The 
 “‘damper-shaped nodules” are, I believe similar to those from which the Wollumbilla 
 and Walsh fossils were obtained. 
 
 1 have within the last year or two received several fine specimens of Crioceras, 
 some in nodules, from Hughenden Township, and in July, 1891, visited the locality a 
 second time. On this occasion Iwas more successful than on the former, having split 
 up many of the “damper-shaped” nodules, each of which was found to contain a 
 Crioceras or other fossil or fossils. There can be no doubt that the nodules are merely 
 concretions occurring in lines along the bedding-planes. 
 
 Mr. George Sweet, of Brunswick, Melbourne, made a collection of fossils from 
 Hughenden in 1889, which have not yet, however, been described.* 
 
 The Rolling Downs Formation occupies the district traversed by the Cloncurry 
 Road from AV onenler above Hughenden, to Fisher’s Creek, near Cloncurry. 
 
 Eight miles below Hughenden, I saw some oval nodules of limestone, one of 
 which, on being split up, was found to be full of fragmentary shells. 
 
 Between fifteen and thirty-nine miles west of Hughenden, frequent outerops 
 were seen of nodular calcareous sandstone (which had for the most part, when 
 weathered, lost its lime) and of flaggy, fine-grained, pale-brown, tough sandstone. 
 
 Thirty-nine miles below ueenelay a gully falling into the left bank of the 
 Flinders exposes horizontal beds of brown sandstones, with Belemnites and small shells, 
 which, however, were not in preservable condition. 
 
 Seven miles above Marathon Station, a limestone bed yielded Awucella hughen- 
 denensis, Eth., Inoceramus pernoides, Eth., and the wing of a Neuropterous insect, 
 Aischna flindersensis, Woodward.¢ One bed of limestone was entirely made up of 
 fragments of Inoceramus. 
 
 At Marathon Station I saw ie beds of fine-grained buff-yellow sandstone, 
 shales, and limestone referred to by Daintree as the source of his fossils, but in 
 the time I could spare (1 was hurrying to join the Transcontinental Railway 
 Expedition under General Feilding, at Cloncurry, in the year 1881) I could find 
 no fossils well enough preserved to take away, but I saw numerous tragments of 
 Inoceramus. 
 
 ‘Seven miles below Marathon Station I obtained specimens of Inoceramus (of 
 the remains of which one bed was entirely composed) from buff-coloured and reddish 
 calcareous sandstones. 
 
 * This Collection has now been partially examined (May, 1892), and a few of the results are 
 incorporated in subsequent pages of this work. The whole will be stihsequently described with other 
 material officially collected in the meantime. (R. ZH. Junr.) 
 
 + On the Wing of a Neuropterous Insect from the Cretaceous Limestone of Flinders River, North 
 Queensland. By Henry Woodward, L,LD., F.R.S., Geol. Mag. (1884), vol. i., p. 337. 
 

 
 400 
 
 Twenty-five miles below Marathon Station the road began to be strewn with 
 “cone-in-cone”’ limestone, evidently derived from beds in situ beneath, and from one 
 to four inches in thickness. About a mile further I saw fine-grained yellow sandstones 
 and grey shales dipping at 7° to the S.E. 
 
 Three miles above Richmond Downs I observed the following section :— 
 
 ft. in. 
 Shales, say _.. aes te is af a oti a re a) 
 Soft grey and yellow sandstone ... ct ae Pes ss Aree re Aw) 
 Limestone A me Se fas Se oe ee an vee eee 
 
 The bottom of the limestone had a cone-in-cone structure, and the top was full 
 of shells, which my Colleague named Jnoceramus Carsoni, McCoy, I. Sutherlandi, McCoy, 
 and Inoceramus, a third species. Daintree’s observation, already quoted, that the 
 cone-in-cone limestone contains no fossils, and has the appearance of a chemical 
 precipitate rather than that of a mechanical deposit, will be remembered. I saw an 
 Inoceramus quite a foot in length, but was unable to detach it from the matrix. 
 
 Between Richmond Downs Station and the Flinders, yellow sandstones haying a 
 slight dip to the south-east were observed. In similar sandstone below the stockyard 
 I found an Inoceramus. Near the Richmond Downs Post Office I saw a fragment of an 
 immense Crioceras lying on the roadside. 
 
 Thirteen and a-half miles below Richmond Downs Station a gully falling into the 
 left bank of the Flinders exposed a section of crumbling grey and bluish shales with 
 limestone and grey calcareous sandstone. From these I obtained specimens of 
 Inoceramus Carsoni, McCoy. 
 
 Twenty-one and a-half miles below Richmond Downs Station, a gully on the left 
 bank of the river showed a scarp of about twenty feet of brown shales, overlaid by grey 
 sandstones, with an apparent dip (though undulating) up the river. From the shales I 
 obtained Inoceramus Sutherlandi, McCoy. 
 
 Eight miles further the bed and banks of the Flinders expose a series of blue- 
 grey shales and thin-bedded and flaggy soft fine-grained blue-grey sandstone, 
 dipping about 3° to the E. In the sandstone I saw only a fragment of a large flat 
 bivalve. 
 
 At the crossing of Neelia Creek I found Awcella hughendenensis, Eth., and 
 Inoceramus in a bed of limestone. Brown sandstone and cone-in-cone limestone are 
 seen at the crossing. 
 
 For sixteen miles beyond Neelia Creek the road is covered with loose blocks of 
 grey sandstone and cone-in-cone limestone. Belemnites are occasionally seen on the 
 surface. On some ridges sixteen miles from Neelia Creek, I saw sandstone and cone-in- 
 cone limestone dipping slightly to the east. 
 
 Between Neelia and Julia Creeks, grey and brown sandstone and cone-in-cone 
 limestone are frequently seen. At Julia Creek I found-the Gasteropod named Watica 
 Jackii, Eth, fil., and a fragment of a Cephalopod. 
 
 Sections of brown flaggy sandstone and cone-in-cone limestone are exposed by 
 Box Creek. 
 
 One mile west of the Williams River is an outcrop of semi-vitreous sandstone 
 containing Belemnites and nodules of limestone resembling “curling stones’’ in size and 
 shape. _ 
 
 Eight miles beyond the Williams are blocks of avery hard brecciated siliceo- 
 calcareous stratified rock, from which I obtained Jnoceramus. Portions of the rock were 
 almost entirely made up of the disintegrated shelly fibres of this genus. Ialso observed 
 in one piece the impression of a Belemnite. 
 
401 
 
 Fifteen miles from the Williams (on Fisher’s Creek waters), sandstones composed 
 almost entirely of the fibrous shelly matter of Znoceramus are seen to rest on hardened 
 black slates and Lydian stone. Indeed, in several places, notably near Marathon, 
 I noted the presence of beds almost entirely composed of this fibrous material, sufficient 
 to attest that this mollusc must have lived in almost incredible numbers. 
 
 I believe the strata above described, from Wongalee to Fisher’s Creek, near 
 Cloncurry, to form one continuous series. They seem to form a large synclinal trough, 
 with an axis crossing the Flinders from east to west, somewhere in the neighbourhood 
 of Marathon. At the heads of the Flinders the lowest beds do not crop out, as the 
 Rolling Downs Formation there overlaps the Paleozoic and Metamorphic rocks of the 
 Dividing Range, and are covered by the Desert Sandstone and the basalts of the table- 
 land. To the west of Richmond Downs, however, a gentle rise to the west brings up a 
 series of strata which apparently occupy a lower horizon than those in the centre of the 
 trough. From Hughenden to Marathon the strata consist for the most part of grey 
 shales with nodules of magnesian limestone and grey and brown sandstones, which are 
 oceasionally caleareous and nodular. Near Richmond Downs, where an easterly dip is, 
 for the first time, distinctly observable, the limestones assume a different character, and 
 are distinguished by a prevalent cone-in-cone structure. Further west there are fewer 
 shale beds and thicker and browner sandstones. The latter are extensively veined with 
 gypsum, and I have been informed by squatters and others that beds of gypsum are 
 frequently met with in sinking wells. The whole series is fossiliferous.* 
 
 A bed of gypsum, of workable thickness, and of great purity, occurs at Chollarton, 
 near Collingwood. Specimens of this have been presented to the Geological Survey 
 Collection by Mr. Julius von Berger. 
 
 Tbe return journey from the Transcontinental Railway Expedition, from Clon- 
 curry to Charters Towers, vié Cloncurry, Winton, and Rockwood (1881-2), afforded me 
 opportunities of observing the Rolling Downs Formation on a course to the south of 
 that of the outward journey. 
 
 From Edington Station to the head of Eastern Creek scarcely a section of the 
 strata was seen, although the shale dédris and the marked features of the Rolling Downs 
 sufficiently attested the presence of the formation to which they give their name. The 
 divide between the Gulf waters and those of the Great Australian Bight (Diamentina 
 River ?) was crossed imperceptibly, as it forms no “range” whatever. 
 
 One and a-half miles down the Diamentina, from Kynoona Station, some grey 
 and buff sandstones, cone-in-cone limestone, and grey shales were observed. The 
 sandstones contained Echinus spines. 
 
 For the next twenty-five miles down the river, wherever the rock was visible it 
 was found to be of grey or buff sandstone. Sometimes the ground was strewn with 
 large, not well-rounded pebbles of tough quartzite, occasionally inclining to opalization, 
 and smaller and better-rounded pebbles of sandy-brown ironstone. These pebbles are 
 probably derived from the Desert Sandstone, cliffs of which are seen to the south. 
 
 For six miles up and five down the river, from Dagworth Old Station, sandstones 
 with grey sandy shales prevail, and the sandstones get coarser in grain and greyer in 
 colour as the river is followed down. A good deal of silicified wood is seen on the surface; 
 but it is doubtful whether it came from the Rolling Downs Formation, or from the 
 Desert Sandstone, which must have covered it. — 
 
 * Report by R. L. Jack on the Geolugical Features 0 part o the District to be traversed by the pro- 
 posed Transcontinental Railway. Brisbane: by Authority: 1885 Supplemented by Notes made on the 
 Journey and hitherto unpublished, 
 
 23 
 
402 
 
 Between the Diamentina and Wokingham Creek, grey sandstones are seen at 
 intervals, with occasional sandy ironstone or ironmasked sandstone.  Silicified wood is 
 strewn over the soil. 
 
 On Watts’ Creek, a tributary of the Diamentina, pale greenish-grey sandstones 
 are seen in thick beds. The sandstone has a remarkable internal structure. Although 
 the lines of bedding continue without interruption, a concretionary process acting on 
 the protoxide of iron in the rock appears to have hardened spherical portions of the 
 mass, which can easily be detached from the softer portions. These spheres weather out, 
 as round as cannon-balls, and can be seen in the bed of the creek, of all sizes, from that 
 of small shot to six feet in diameter. I have so frequently heard descriptions of similar 
 “sandstone balls”? from different portions of the Rolling Downs, that the structure 
 referred to cannot be uncommon, but the above is the only instance I have seen. The 
 *balls”’ are not waterworn, it must be remembered, but concretionary. 
 
 In a well sunk, about 1878, on the march between Werna and Ayrshire Downs 
 Runs, a three to four inch seam of coal was cut at one hundred and forty feet; a 
 second seam was struck between one hundred and forty feet and one hundred and 
 eighty feet. The sinking was left off in hard fine-grained sandstone at two hundred and 
 four feet. I was informed that the strata passed through were, with the exception of 
 the coal-seams, all grey sandstones and sandy shales, and that among the beds cut 
 through were an argillaceous flagstone with shells and several beds of sandstone with 
 iron pyriies, and that many fragments of silicified and carbonised wood were met with. 
 Some fragments of coal from the spoil-heap gave, on an approximate analysis :— 
 
 Carbon oe one a Ae As, nn se ot Peo O7, 
 Volatile vee ei ar ne sae tf 25; 2. se 06396 
 INCU, eae ae Ae 5c sey AA ae a on eco) 
 
 100°00 
 
 This coal does not soil the fingers, and bears a close resemblance in composition 
 to the famous Lesmahagow Cannel Coal, although it is brighter and more lustrous in 
 cross fracture. My samples had lain exposed to the weather for two and a-half years, 
 and must have lost some of their volatile matter. An analysis of the Lesmahtagow Coal 
 is given for comparison :— 
 
 Carbon HAR wae oe ah a Sot Ane — Mee tg) 
 Volatile nie sn APC oe a ae ar we ee wo:60 
 PN et par Be Aap ae bef eh =a ee acm ... 400 
 
 100°00 
 
 A little water was struck below the first coal-seam, and a little at one hundred 
 and eighty feet. Water stood at one hundred and thirty-four feet from the surface. 
 
 In the Township of Winton, “ Sheppard’s Well” was sunk in Allotment 7 of 
 Section 1. Mr. Julius von Berger supplied me, in 1882, with the following 
 section :— 
 
 Ft. in. 
 Alluvial layer (yellowish, sandy, with a few seams of 
 carbonaceous ash) 40 O 
 Coaly shale O 0f 
 Second alluvial layer 40 0 
 Coal-seam . ss oy “fe a as sc Ay emt. 
 Third alluvial layer (compact clay-shale with pieces of jet 
 and lanceolate leaves : in the middle of the layer a bed 
 of shells) ie =e ay ae ey, a ee Ae) 
 Coal-seam ... at 04 ae ae we sau ssi Po 
 Hard alluvial clay ss oe a ee re rey EK 8] 
 
403 
 
 No water was obtained in the well. The following analysis of some of the 
 coal fragments from the spoil-heap was made on my return to Townsville :— 
 
 Carbon aga “oF He sf aAe AS ae vee ». 30°32 
 Volatile a0 rae it Pee ra Sea fe ae we =49°34 
 TA Shion rc ey! Ar: sae aa Mae a6 Bae ... 20°34 
 
 100:00 
 
 Another well was sunk by the Government, just behind the Court House in 
 Winton, but owing to the recent sudden death of the contractor I could get no informa- 
 tion as to the strata passed through. I found (2nd January, 1882) that the greater 
 part of the shaft was slabbed up, but I was informed that a coal-seam fifteen 
 inches in thickness was cut at seventy feet, and another at about one hundred feet. At 
 the bottom of the shaft (one hundred and fifty feet), where it was still unslabbed, I saw 
 horizontally bedded sandy shales. The coal-seams were fifteen and twenty-four inches 
 in thickness respectively. That is, I came to that conclusion, for the accounts I got 
 differed considerably. Opinions would naturally differ as to how much was coal and 
 how much shale. From the fragments I picked up in the spoil-heap, I should say that the 
 coal occurred in thin layers among dark carbonaceous shales. Specimens I analysed at 
 Townsville gave— 
 
 
 
 Carbon Bor ae ame pa eo Se 56 ies w 02°49 
 Volatile aa ie ee Rie ee es; S “rr vee =42°93 
 Ash ooo eee vee eee eee eee eee eos wee eee 4°58 
 
 100°00 
 
 Two species of the genus Unio from this well were presented to the Geological 
 Survey Museum by Mr. Julius von Berger.* 
 
 On Vindex Station, near Winton, a well was sunk about 1880. As the station 
 had changed hands between that time and the date of my visit (8rd January, 1882), I 
 could get little information, but I learned that a nine-inch coal-seam was cut at seventy- 
 five feet, and other two seams (the upper one sixteen inches thick) between seventy-five 
 and one hundred feet. At one hundred and ten feet a sufficient supply of water (which 
 rose twenty-five feet) was struck, and the sinking was stopped. The rubbish round the 
 well consisted of soft grey shales and flags, with chips of coal, and a few lumps of hard 
 buff-coloured sandstone. 
 
 ~ A second well was sunk on Crawford’s Creek, nine miles east of Vindex, and 
 water was obtained at one hundred and fifty feet. The strata passed through were very 
 much the same as in the well at the station. I heard that coal had been passed through, 
 but could get no reliable information. 
 
 A twelve-inch bore was being sunk by Mr. F. de Kock on Vindex Run, about 
 seven miles N. 15° E. of the station. I had previously seen, in Mr. von Berger’s 
 hands in Winton, samples of some of the strata labelled according to their depths. Mr. 
 de Kock supplied me with the latest particulars of the boring :— 
 
 Feet. 
 Surface ... he se oe wa se so ar BAe eine 
 Fine-grained, soft, friable, buff-coloured sandstone -. ee Pe 45 
 Loose ground _... wie re yi9 oe sas ove ny 2 alt 
 Yellowish sandstone, hard and fine-grained, with silicified wood below... 7 
 Loose ground ,.. oh “ te oat kod ep a caw 
 
 * A deposit of Unio has been met with by Prof, R. Tate in the Lake Eyre Basin, South Australia. The 
 specimens have been examined by my Colleague, 
 
4:04 
 
 
 
 Feet. 
 ( Blue clay, with a little fine siliceous sand ... aw 6 
 | Stiff brown plastic clay, with a little hard bluish clay, with plant- 
 impressions ... =a site = 2 
 Ngee: of pale pyrites from depths of NEA ae ie xP 120. 139 
 Coal, 2 feet thick at 130 feet deep... ze t he a coke & 
 Damp Hard grey sandstone ... ar Hs mes 4 i 
 Coal, 2 feet thick united with sandy clay, vi ie age Be pee oO 
 Sandy clay, carbonaceous, down to ... dna ses ae one cae 8 
 Fine-grained sandy clay (very wet), to 7. 3 pis np we 5186 
 Hard grey sandstone, to Pa a ss - ne : we L87, 
 
 Grey sandy clay. 
 
 At the “ Stone Hut,” on Rockwood Creek, is a bed of grey sandstone weathering 
 buff, the lowest four inches of which is a sort of conglomerate of curious long oval 
 pebbles of clay, which I think must be rolled casts of Lingula-like bivalves, together with 
 fish-teeth, Echinus spines, Belemnites, Gasteropods, and Pelecypods. Among thespecimens 
 which I brought home, my Colleague recognised fangs and tooth of Otodus, Belemnites, 
 Aucella hughendenensis, Eth., and sections of long spiral univalve shells. 
 
 Half-a-mile east of Byrinnia Station are some quarries of blue-grey sandstone 
 weathering buff, containing some shells. 
 
 From Rockwood, on the Landsborough, grey sandstones and drab-coloured lime- 
 stones are seen at intervals for sixteen miles, when, at the “Jump Up” on the head of 
 Jirking Creek, the Desert Sandstone unconformably overlies the Rolling Downs 
 Formation. 
 
 From the Junction of Rockwood Creek with the Landsborough, my Colleague 
 recognised Inoceramus (a young form) among my Collection; from the Landsborough, 
 five and a-half miles north-north-west of Rockwood, Awcella hughendenensis, Kth., 
 and Pecten; and, from near the head of Jirking Creek, Awcella hughendenensis, Eth., 
 and Pecten. In the same district numerous examples of Jnoceramus were seen on the 
 ground, but they were either too bulky, or too imperfect, to carry away. 
 
 During a journey in the southern part of the Western Interior, in October and 
 November, 1885, accompanied by Mr. J. B. Henderson, Hydraulic Engineer, I made the 
 following notes :— 
 
 At Minmi Old Station, on Bungil Creek, near Roma, a soft dull-grey sandstone, 
 with thin partings of blue shale, dips to 8. at 2° to 3°. The sandstone contains 
 numerous plant-impressions, some fragments of silicified wood, and fossil Pelecypoda, 
 of which a list is given on a subsequent page. 
 
 On the Maranoa River, about half-a-mile north of the Railway, are blue shales 
 with bands of limestone nodules. The shales and limestone at the lowest point down 
 the river dip wp the river at about 15°. The remainder of the section dips, if 
 anything, up the river, but is practically horizontal. From the limestone noduies I 
 obtained numerous fossils, among which my Colleague recognised the Pelecypoda, of 
 which a list is also given on a subsequent page.* 
 
 On Yo Yo Creek, a tributary of the Warrego, in Lat. 26° S., is a section 
 of green sandstone with calcareous and ferruginous parts, and grey shales, and 
 cone-in-cone limestone in very thin bands. Ironstone nodules in the shale contain 
 doubtful leaf-impressions and shells, and the sandstone contains Belemnites. The 
 Rolling Downs rocks are seen’at intervals between Yo Yo Creek and Ellangowan. 
 
 
 
 *Tna collection from the Lake Eyre Basin, submitted by Prof. R. Tate to the undersigned, an 
 exactly similar matrix and mode of preservation of the fossils exists, (R. Z, Junr.) 
 
405 
 
 On the Nive River, at the Royal Hotel, grey shales with indistinct plant+ 
 remains, accompanied by greyish-green sandstone and cone-in-cone limestone, dip to S. 
 at about 1°. 
 
 In the neighbourhood of Tambo the country forms extensive “downs,” with 
 here and there blocks of sandstone, soft and not very coarse-grained, yellow near the 
 outside and green in the interior. The sandstone is pierced with round holes at right 
 angles to the bedding-planes. The holes occur too sporadically and are too deep to be 
 ‘ rain-drops. The sandstone has, apparently, all been calcareous, and occasionally has 
 films of half-an-inch to three inches of cone-in-cone limestone adhering to it. 
 
 Nine miles down the Bareoo River from Tambo, a calcareous sandstone 
 was observed, crammed with Belemnites and other fossils, including Zrigonia. An 
 exactly similar rock was seen four miles further down the river. 
 
 Six miles below the Northampton Hotel, on the Barcoo, a stony ridge on the 
 right bank of the river contained large and small round and roundish nodules of limestone. 
 In the centre of each of the smaller nodules is a shell, while the interiors of the large 
 nodules are, for the most part, shapeless masses of red iron ochre. ‘The shells are 
 mainly Aucella hughendenensis, Eth. 
 
 Five miles below Northampton Downs Station, a white limestone is seen on a 
 small hill-top. Ina gully on the west side of the hill is a section of grey shales and 
 brown sandstones underlying the limestone of the hill-top. These strata bave a sight 
 dip to east-north-east. The sandstone contains a few shells. 
 
 At Blackall, the town well, two hundred and fifty feet deep and unsuccessful, 
 passed through grey-green flaggy sandstone, a bed of cone-in-cone limestone, and grey 
 shales, containing bivalve shells and Belemnites. The bivalves have their shelly matter 
 converted ito carbonate of lime, and crumble very readily. 
 
 Between Blackall and Aramac, seven miles from Skeleton Creek (in “ Recovered 
 South” Block), brown sandstones dip at 5° to S. 
 
 Two miles beyond Home Creek Station a cone-in-cone limestone is met with. 
 
 At Coreena Wool-shed, twenty-one miles north of Saltern Creek, a drab-coloured 
 limestone yielded numerous examples of Aucella hughendenensis, Eth. 
 
 At Aramac,a well had been sunk to the depth of three hundred feet by the 
 Divisional Board. From specimens preserved by Mr. S. Sharwood, and the information 
 that gentleman afforded me, I constructed the following section :— 
 
 At 22 feet.—Yellow clay shale. 
 
 30 feet.—Yellow clay shale more sandy. 
 
 » 36 feet.—Two veins of gypsum. 
 
 45 feet.—Alternate shale and fine sandstone. 
 
 47 feet.—Fine-grained permeable sandstone, felspathic, siliceous, and micaceous. 
 Salt water in this. 
 
 60 feet.—Clay shale, black films of plant-impressions and impressions of shells, 
 
 70 feet.—Clay shales with shells and pyrites concretions. 
 
 78 feet.—Clay shales, a little sandy. 
 
 », 83 feet.—Clay shale. 
 
 90 feet.—Clay shale. 
 
 ,, 110 feet.—Clay shale and a concretion, in part calcareous. 
 
 », 112 feet.—Clay shale. 
 
 », 128 feet.—Clay shale. 
 
 132 feet.-—Clay shales with shells (unaltered) and pyrites. 
 
 150 feet.—Sandy clay shales. 
 
 153 feet.—Sandy clay shales. 
 
 176-8 feet.—Sandy clay shales, and a calcareous sandstone nodule. 
 
 +] 
 
 9 
 
 33 
 
 ”? 
 
406 
 
 At 212 feet.—Clay shales with shells and a limestone nodule. 
 * At 224 feet.—Grey fine-grained sandstone with Ancyloceras Flindersi, McCoy. 
 », 232 feet.—Clay shales. 
 »5 235 feet.—Clay shales with shells. 
 * At 238 feet.—Clay shales with Inoceramus Crispii, Mantell?, Belemnites Canhami, 
 Tate, and Ancyloceras Flindersi, McCoy. 
 * At 244 feet.—Clay shales with Inoceramus Crispii, Mantell ?, <Aucella hughen- 
 denensis, Eth., Nucula quadrata, Eth., and Nucula, sp. ind. 
 * At 284 feet.—Limestone nodule with Crioceras, sp. ind. 
 * At 290 feet.—Clay shale with Ammonites Flindersi, McCoy. 
 
 The fossils to which an asterisk (*) is attached were presented to the Geological 
 Survey Museum by Mr. Sharwood, and identified by my Colleague. 
 
 The reluctance to admit that the Wollumbilla fossils had really been found 
 in situ, and the refusal to take into consideration Mr. N. Taylor’s Walsh fossils, on the 
 ground that they occurred in drifted boulders (whereas they occurred in concretionary 
 nodules), resulted naturally enough from the presence of an assemblage of fossils such 
 as in Europe could not have occurred in any one formation. It is remarkable that 
 almost every Paleontologist who has worked hitherto on Queensland materials has come 
 to the conclusion that fossils from different localities have been mixed up, and this 
 explanation has appeared to be specially necessary in the case of fossils from the 
 Rolling Downs. On the other hand, my own explorations have satisfied me that 
 Queensland fossils are not more liable to this kind of accident than those of other 
 countries ; that the mixing-up which has caused so much annoyance to Palzontologists 
 has been perpetrated by Nature herself; that we have a continuous series of beds of 
 enormous thickness, in which, however, from the scarcity of sections, it would be 
 impossible to map out “horizons”; and that the fossils of the Rolling Downs, from 
 the Gulf to the New South Wales Boundary,* must be treated asa whole. Shading 
 gradually upwards from the plant-bearing Ipswich Beds, the Rolling Downs Formation 
 contains a marine (and occasionally freshwater) fauna, representing the migration of 
 many species which in Europe date from Rhetie to Cretaceous, but which cannot be 
 quoted as arguing a strict contemporaneity of life. 
 
 Although mainly a marine deposit, plant-beds and coal-seams, indicating fresh 
 water or terrestrial conditions, are by no means rare. At one time Iindulged the hope 
 of being able to separate a Lower, or Marine, from an Upper, or Freshwater Series,t 
 but later experience has convinced me that this is impracticable, plant-beds and coal- 
 seams being met with at different horizons, and not being identifiable over large areas. 
 It may be said that I have not myself seen a single plant in the Rolling Downs in 
 determinable condition, the shales on which they are imprinted crumbling rapidly on 
 exposure. The Hon. A.C. Gregory, however, mentions} that many well-preserved speci- 
 mens of ferns, including Teniopteris and Pecopteris, were found in an ironstone bed in 
 Bungeeworgorai Creek, ten miles above the main Western Road; and a specimen 
 labelled Sphenopteris, from the Bulloo River, in the south-western corner of the Colony, 
 is included in the collections of the Queensland Museum, Brisbane. 
 
 In addition to the localities already enumerated, coal has: been found in the 
 Rolling Downs Formation at Malta, east of Tambo (three seams in thirty-six feet, one 
 seam three and a-half feet thick); at the head of Bungeeworgorai Creek, north-east of 
 Mitchell (a thick seam) ; and at Dulbydilla, on the Western Railway. 
 
 
 
 
 
 * And those from the Lake Eyre Basin in South Australia. See ‘ Age of the Mesozoic Rocks of 
 the Lake Eyre Basin.” By Prof. R. Tate, Proc. Austr. Assoc. Adv. Sci. (1888), i., p. 228. 
 
 + Transcontinental Railway Report, by R.L.J. Brisbane: by Authority: 1885. 
 
 + Report on the Search for Coal between Dalby and Roma. Brisbane: by Authority: 1879. 
 
407 
 
 Although, as has already been said, the fauna of the Rolling Downs must be 
 treated as a whole, as must also its flora should determinable specimens be obtained, in 
 the following list the various fossiliferous localities hitherto exploited are kept apart, asthe 
 distinction may be found to have some possible utility in the future. The list is intended 
 
 _ by us to correct and supersede all previously published lists. A considerable number of 
 fossils are now recorded for the first time, my Colleague haying carefully worked over an 
 immense mass of material, which I was able to place in his hands, in addition to collec- 
 tions made by Mr. G. Sweet, and Mr. C. W. De Vis from Queensland, other fossils from 
 the north-west corner of New South Wales in the Mining and Geological Museum, 
 Sydney, and a collection obligingly forwarded on loan by Professor R. Tate, from the 
 Lake Eyre Basin, South Australia. The Geological Survey Collection includes valuable 
 donations of Rolling Downs fossils by the following gentlemen:—The Hon. A. C. 
 Gregory, Brisbane; Messrs. J. B. Henderson, M.I.C.E., Hydraulic Engineer, Brisbane ; 
 R. Sexton, C.E., Brisbane; J. Falconer, Brisbane ; the late James Smith, Rockhampton ; 
 E. K. Ogg, Rockhampton ; Goffage, Tambo; Rowland Morrisby, Blackall; S. 
 Sharwood, Aramac; B. R. Edkins, Mount Cornish; Julius von Berger, Winton; G. Cramieri, 
 Winton; P. F. Sellheim, Gympie; R. Sefton, Townsville; W. Landers, Townsville; A. 
 Brand, Townsville; A.C. Macmillan, C.E., Ayr; R. Gray, Hughenden; J. Burkitt, 
 Maxwellton, near Hughenden; J. Hugh Moor, Manfred Downs, near Cloncurry ; 
 P. W. Pears, Normanton ; the Rev. T. W. Ramm, late of Hughenden; W. L. Mackinnon, 
 A.M.1.C.E., Irrigation Engineer, Brisbane ; and D. P. Ryan, Hughenden. 
 
 Among the most interesting of these donations are portions of skeletons of 
 Ichthyosaurus and Plesiosaurus (?), to which my Colleague refers in his Notes. The 
 former is from the bed of the Flinders, thirty-five miles below Richmond Downs (Mr. 
 J. Burkitt) ; Flinders River, at Manfred Downs (Mr. J. Hugh Moor); and Flinders 
 River, near Glendower (Mr. W. L. Mackinnon). The latter is from Manfred Downs 
 (Mr. J. Hugh Moor). 
 
 We are indebted to Mr. C. W. De Vis for an opportunity of examining a portion 
 of an Ichthyosaurus from Marathon Station, on the Flinders, and vertebre of Plesiosaurus 
 from the Walsh River. The specimens are in the Queensland Museum.* These 
 fossils confirm the previous determination of such genera made by Prof. McCoy, and, 
 from their strong Cretacious facies, assist in approximately fixing the age of the deposits 
 in which they occur. 
 
 Another very remarkable fossil is a fragment of a Ganoid fish, measuring about 
 ten inches square, from Hughenden, presented by Mr. D. P. Ryan. This fish is speci- 
 fically identical with that first discovered by Mr. George Sweet, of Brunswick, Melbourne, 
 in the Rolling Downs, near Hughenden, and named Belonostomus Sweeti. It is described 
 by my Colleague and Mr. A. Smith Woodward as ‘‘ the largest species of the Mesozoic 
 Ganoid Belonostomus which has yet been found. ‘The fish lived in the same geological 
 period, in Western Europe, India, and Brazil, and the’ present discovery is thus of 
 great interest, as extending still further the ascertained geographical range of this 
 genus during Mesozoic times.” 
 
 In the southern portion of the area watered by the Warrego, Paroo, and 
 Cooper’s Creek, there is a great thickness of the “ Rolling Downs” strata, but it is 
 probable that the uppermost beds are frequently débris of the Desert Sandstone accumu- 
 lated ona continental land surface during Tertiary times. In this region the thick brush- 
 wood of mulga and gidyah forms a strong contrast to the open downs. This subject will 
 be further referred to in treating of the Moondilla gold discoveries, in Chapter XXXV. 
 
 
 
 * See R, Etheridge, Junr., Proc, Linn. Soc. N.S. W., 1889, Vol. iii, Pt. 2, pp. 405 and 410, 
 
408 
 
 An admirable description is given of the Rolling Downs Beds, as they are 
 developed in South Australia, in a Paper on “The Mesozoic Plains of South Australia,” 
 by Mr. H. Y. Lyell Brown, Government Geologist of that Colony, read before 
 the Australasian Association for the Advancement of Science,* from which a few 
 extracts may with advantage be made in this place. 
 
 “The area over which the Mesozoic beds form the surface rock, or are only 
 thinly covered by those of Tertiary formation, extends east from the boundaries of 
 New South Wales and Queensland, westward to the boundary of Western Australia ; 
 northward it is bounded by the Musgrave Ranges and Lat. 26°, and southward by 
 an irregular line extending from the northern edge of the Nullarbor Plains in Western 
 Australia, round by the Warburton Range and the northern extremity of the main 
 range to the vicinity of Lake Frome, near which it passes into New South Wales. 
 Here and there along the telegraph line from Hergott Springs to the Peak and 
 Charlotte Waters, the Dennison, Margaret, and other ranges, composed of Primary 
 rocks, protrude through it in the form of islands, rising above the ‘general surface in 
 places to a height of 1,000 feet or more.” . . . . “The general level of this vast 
 territory varies from some two hundred feet above sea-level to twenty five or thirty feet 
 below it, in the case of Lake Eyre.” 
 
 After describing the “Table-land and Table-hill country” and the “Stony 
 Downs,” which he refers to as “ either of Upper Cretaceous or Lower Tertiary age,” 
 Mr. Brown continues as follows :— 
 
 “Below and surrounding the table-hills and stony downs, are the soft silt 
 plains, which, together with the former, cover the gypseous clays, marls, calcareous 
 shales, limestones, sand, and gravel drifts of Cretaceous age. The greatest thickness 
 of these beds, which has been proved by boring at Tarkininna, is about 1,200 
 feet.” . . . . “Bores have been sunk by the Government in this forma- 
 tion at Tarkininna, where artesian water was tapped at 1,200 feet, and at 
 Hergott, Coward Springs, Strangway Springs, &c., where a large supply of water 
 was attained at an average depth of some three hundred feet. The supply from 
 some of these bores is over a million gallons per day.” . . . . “The fossils which 
 occur in this formation are found in masses and nodules of limestones, and in the 
 calcareous shales, but generally they are most plentiful in the former, which are often 
 entirely composed of them.”’ 
 
 It is very satisfactory to have our long-entertained view of the age of the 
 Rolling Downs Formation of Queensland confirmed, as regards the extension of the 
 same formation into South Australia, by such a competent authority as Prof. Ralph Tate, 
 of Adelaide, who, in a Paper ‘On the Age of the Mesozoic Rocks of the Lake Eyre 
 Basin,” + makes the following remarks :— 
 
 “The occurrence of Crioceras and a Ceratite-like Ammonite among the common 
 fossils of the Lake Eyre Basin demands their relegation, as also those of Wollumbilla, 
 to the Cretaceous System;” and again :—“ The European identities alleged to oceur in 
 the Wollumbilla beds, are Lingula ovalis, Avicula braamburiensis, Belemnites paxillosus, 
 Serpula intestinalis, and Rhynchonella variabilis. Relying on Mr. Moore’s determina- 
 tions, I have persistently advocated the Jurassic age of the Lake Eyre fossils ; but, 
 forced to abandon that position by the more decided Cretaceous facies of recently 
 acquired species, it becomes necessary to reinvestigate the claims of the fore-mentioned 
 species to bear the names attached to them.” 
 
 * Proc. Austr. Assoc. Adv, Sci., 1888, i., p. 241. 
 t+ Ivid., p. 228. 
 
409 
 
 Professor Tate then gives the following list of Cretaceous fossils from the Lake 
 
 Eyre Basin :— 
 
 
 
 Species. 
 
 
 
 Crioceras australe, Moore 
 Belemnites australis, Phillips 
 
 5 Canhami, Tate 
 
 Ss Sellheimi, Ten. Woods 
 
 eremos, Tate .. 5 
 
 Cinulia Hochstetteri, Moore 
 Natica variabilis, Moore 
 
 (Natica lineata, Eth.) 
 
 Dentalium arcotinum, Forbes (Dentalium lineatum, Moore) 
 
 Other Occurrences. 
 
 Upper Maranoa. 
 Grey Range ; Wollumbilla. 
 
 Palmer River, 
 Wollumbilla. 
 Wollumbilla. 
 Wollumbilla ; Mary- 
 borough.* 
 Wollumbilla; India. 
 
 Avicula Barklyi, Moore (Avicula reflecta, Moore ; Avicula orbicularis, Grey Range; Wollumbilla. 
 
 Hudleston) 
 Avicula umbonalis, Moore 
 cor biensis, Moore 
 
 Aucella hughendenensis, Eth. (Aucella Liver sidgei, Eth. junr. ) 
 
 Cytherea Clarkei, Moore (Cyprina expansa, Eth.) 
 
 Cytherea Woodwardiana, Hudleston 
 Gervilleia angusta, Hudleston 
 
 Mytilus inflatus, Moore (Mytilus linguloides, Hudleston) ... 
 »  rugocostatus, Moore (Mytilus Scoulari, Tate) 
 
 Myacites MeCoyii, Moore 
 ” 
 Nucula quadrata, Eth. 
 » truncata, Moore 
 Pecten psila, T. Woods (? Pecten socialis, jt, Moore) 
 Trigonia nasuta, Eth. 
 ys lineata, Moore 
 Lingula subovalis, Davidson 
 
 
 
 rugosa, Moore (Myacites australis, Hudleston) 
 
 Wollumbilla. 
 
 Wollumbilla. 
 
 Grey Range ; Hughenden ; 
 Marathon. 
 
 Grey Range ; Wollumbilla; 
 Maryborough.* 
 
 
 
 Wollumbilla; Palmer River. 
 Wollumbilla. 
 
 Wollumbilla. 
 
 Wollumbilla. 
 Maryborough.* 
 Wollumbilla. 
 
 Grey Range ; Wollumbilla. 
 Maryborough.* 
 Wollumbilla. 
 Wollumbilla; England. 
 
 “In addition to the above, are species of :—Ammonifes (with the sutures of Ceratites), Alaria, 
 two sp., Modiola, Natica, Leda, Pecten, Gervilleia, Pinna, Arcomya, Pleuromya, Rhynchonella, and of 
 
 several uncertain genera of bivalves.” 
 
 LIST OF FOSSILS FROM THE ROLLING DOWNS FORMATION IN 
 QUEENSLAND. 
 
 WOLLUMBILLA. 
 FORAMINIFERA. 
 Cristellaria acutauricularis, Ficht. and Moll. 
 Cristellaria acutauricularis, var. longicostata, 
 Moore. 
 Cristellaria cultrata, Montfort, var. radiata, 
 Moore. 
 Dentalina communis, D’ Orb. 
 Vaginulina striata, D’ Orb. 
 Polymorphina gibba, D’Orb. 
 Polymorphina lactea, Walker and Jacob. 
 Planorbulina lobatula, D’Orb. 
 Planorbulina Ungeriana, D’ Orb. 
 SILICISPONGIA. 
 Purisphonia Clarkei, Bowerbank. 
 NEOCRINOIDEA. 
 Pentacrinus australis, Moore. 
 TUBICOLA. 
 Bae puls intestinalis, Phillips. 
 
 
 
 * Desert Sandstone. 
 
 
 
 CIRRIPEDIA. 
 Traces (?) adhering to Panopea. 
 
 Potyzoa (Gymnolemata). 
 Lepralia? oolitica, Moore. 
 
 BRACHIOPODA. 
 Terebratella Davidsoni, Moore. 
 Argiope? wollumbillensis, Moore. 
 Argiope? punctata, Moore. 
 Rhynchonella rustica, Moore. 
 Rhynchonella solitaria, Moore. 
 Discina apicalis, Moore. 
 Lingula ovalis, J. Sowerby. 
 
 PELECYPODA. 
 
 Pecten Moore, Eth. fil. 
 
 Pecten equilineatus, Moore. 
 
 Pecten socialis, Moore. 
 
 Lima Gordont, Moore. 
 
 Lima? multistriata, Moore. 
 
 Lima? braamburiensis (Sby.), Phillips. ? 
 
 
 
 (R.LJ.) 
 
LIST OF FOSSILS FROM THE ROLLING DOWNS FORMATION IN 
 QUEEN SLAN D—continued. 
 
 WOLLUMBILLA—continued. 
 PELECYPODA—continued. 
 
 Oxytoma ? simplex, Moore. 
 Pseudavioula anomala, Moore. 
 Pseudavicula australis, Moore. 
 Maccoyella Barklyi, Moore. 
 Maccoyella reflecta, Moore. 
 Maccoyella? wmbonalis, Moore. 
 Maccoyella ? corbiensis, Moore. 
 Maccoyella? substriata, Moore. 
 Perna gigantea, Moore. 
 Mytilus Tenison-Woodsi, Eth. fil. 
 Mytilus rugocostatus, Moore. 
 Mytilus inflatus, Moore. 
 Modiola unica, Moore. 
 Arca pralonga, Moore. 
 Nucula Cooperi, Moore. 
 Nucula truncata, Moore. 
 Nucula australis, Moore. 
 Trigonia lineata, Moore. 
 Astarte wollumbillensis, Moore. 
 Cyprina Clarkei, Moore. 
 Macrocallista ? plana, Moore. 
 Glycimeris rugosa, Moore. 
 Goniomya depressa, Moore. 
 
 GASTEROPODA. 
 Dentalium wollumbillensis, Eth. fil. 
 Cinulia Hochstetteri, Moore. 
 Acteon depressus, Moore. 
 Delphinula? reflecta, Moore. 
 Natica variabilis, Moore. 
 Natica ornatissima, Moore. 
 
 CEPHALOPODA. 
 Teuthis. 
 Belemnites australis, Phillips. 
 Belemnites eremos, Tate. 
 Belemnites Sellheimi, Ten. Woods. 
 Crioceras australe, Moore. 
 
 BUNGEEWORGORAT CREEK. 
 (Twenty miles south east of Mount Abundance.) 
 
 PELECYPODA. 
 Maccoyella Barklyi, Moore. 
 Maccoyella reflecta, Moore. 
 Maccoyella wnbonalis, Moore. 
 Maccoyella? corbiensis, Moore. 
 Maccoyella? substriata, Moore. 
 Mytilus rugocostatus, Moore. 
 Glycimeris rugosa, Moore. 
 Corimya Wilsoni, Moore. 
 
 AMBY RIVER. 
 NEOORINOIDEA. 
 Pentacrinus australis, Moore. 
 
 
 
 AMBY RIVER.—continued. 
 PELECYPODA. 
 Glycimeris 2 Maccoyi, Moore (between “ Amby 
 and Maranoa Rivers”). 
 Corimya Wilsoni, Moore. 
 BLYTHESDALE. 
 (Fifteen miles from Wollumbilla.) 
 PELECYPODA. 
 Maccoyella Barklyi, Moore. 
 Maceoyella corbiensis, Moore. 
 Tancredia? plana, Moore. 
 GASTEROPODA. 
 Natica variabilis, Moore. 
 
 MOUNT CORBY. 
 PELECYPODA. 
 Maccoyella corbiensis, Moore. 
 
 MITCHELL RAILWAY STATION BORE. 
 PELECYPODA. 
 Pecten? (Pl. 21, Fig. 5.) 
 
 MARANOA RIVER. 
 (Half a mile above Mitchell Railway Station.) 
 PELNCYPODA. 
 
 Maccoyella Barklyi, Moore. 
 Pseudavicula anomala, Moore. 
 Corbicella 2? maranoana, Eth. fil. 
 Glycimeris Tatei, Eth. fil. 
 Glycimeris rugosa, Moore. 
 Gastrochena australis, Eth. fil. 
 
 GASTEROPODA. . 
 Natica variabilis, Moore. 
 
 GORDON DOWNS. 
 (Near Roma.) 
 PELECYPODA. 
 Tancredia ? sp. ind., Eth. 
 Homomya, sp. ind., Eth. 
 
 GASTEROPODA. 
 Pleurotomaria? Cliftoni, Eth. 
 
 MINMTI. 
 (Near Roma.) 
 PELECYPODA. 
 Oxytoma? simplex, Moore. 
 Cyprina Clarkei, Moore. 
 Corimya Wilsoni, Moore. 
 
 MARANOA RIVER. 
 
 PELECYPODA. 
 Pseudavicula anomala, Moore. 
 Pseudavicula australis, Moore. 
 Cyprina Clarkei, Moore. 
 Glycimeris rugosa, Moore. 
 
LIST OF FOSSILS FROM THE ROLLING DOWNS FORMATION IN 
 QUEENSLAN D—continued. 
 
 MARANOA RIVER—continued. 
 CEPHALOPODA. 
 Belemnites australis, Phillips (“ Upper Maranoa 
 River’). 
 Crioceras australe, Moore (“ Upper Maranoa 
 District”). 
 WARREGO RIVER. 
 
 CEPHALOPODA. 
 Hamites ? laqueus, Eth. fil. 
 
 GREY RANGES. 
 (Mount Stewart Run, N.S.W. Boundary of 
 South Australia and Queensland). 
 
 PELECYPODA. 
 Pecten psila, Ten. Woods. 
 Trigonia mesembria, Ten. Woods. 
 
 CEPHALOPODA. 
 Belemnites oxys, Ten. Woods. 
 
 NIVE DOWNS. 
 
 PELECYPODA. 
 Mactra trigonalis, Moore. 
 
 GLANMIRE BLOCK. 
 (North-east end. Seventeen miles south-west of 
 Tambo.) 
 PELECYPODA. 
 Cucullea Hendersoni, With. fil. 
 Cytherea ? Hudlestoni, Eth. fil. 
 GASTEROPODA. 
 Dentalium wollumbillensis, Eth. fil. 
 Actaon depressus, Moore. 
 CEPHALOPODA. 
 Ammonites inflatus, J. Sowerby, var. (Pl. 34, 
 ff. 1-4.) ; 
 BARCOO RIVER. 
 (Six miles above Northampton Downs Station.) 
 PELECYPODA. 
 Aucella hughendenensis, Eth. 
 
 BARCOO DISTRICT. 
 PELECYPODA. 
 Mytilus ingens, Ten. Woods. 
 TAMBO AND BLACKALL ROAD. 
 (Nine miles from Tambo.) 
 PELECYPODA. 
 Trigonia, sp. ind. (b), (Pl. 21, f. 21). 
 CEPHALOPODA. 
 Belemnites, sp. (P1. 35, ff. 15 and 16). 
 
 EVORA STATION. 
 (Twenty-five miles north-east of Blackall.) 
 
 PELECYPODA. 
 Cytherea (Cyprina ?) Mooret, Eth. fil. 
 
 EVORA STATION—continued, 
 
 GASTEROPODA. 
 Anchura ? Wilkinsoni, Eth. fil. 
 
 BARCALDINE. 
 CEPHALOPODA. 
 Belemnites Canhami, Tate. 
 Ammonites Flindersi, McCoy (at Railway 
 Station). 
 Hamites ? laqueus, Eth. fil. (on Wellshot Run). 
 Nautilus Hendersoni, Eth. fil. (from Barcaldine, 
 and also from Ilfracombe). 
 
 COREENA WOOLSHED. 
 PELECYPODA. 
 Aucella hughendenensis, Eth. 
 
 PITCHERY CREEK. 
 (Barrington’s Station, Central Queensland.) 
 
 REPTILIA. 
 Plesiosaurus Sutherlandi, McCoy. 
 
 MOUNT CORNISH. 
 (Well seven miles east of Station.) 
 
 PELECYPODA. 
 Inoceramus pernoides, Eth. (at 200 feet). 
 
 CEPHALOPODA. 
 Crioceras Edkinsi, With. fil. (at 230 feet). 
 
 ARAMAC. 
 PELECYPODA. 
 
 Pecten, sp. ind. (Pl. 21, ff. 7 and 9). 
 
 Oxytoma rockwoodensis, Eth. fil. 
 
 Aucella hughendenensis, Eth. (in well at 244 
 feet). 
 
 Inoceramus Crispii, Mantell ? (in well at 238 
 and 244 feet). 
 
 Nucula quadrata, Eth. (in well at 244 feet). 
 
 Nucula, sp. ind. (in well at 244 feet). 
 
 Glycimeris aramacensis, Eth. fil. 
 
 CEPHALOPODA. 
 
 Belemnites Canhami, Tate (in well at 238 feet). 
 
 Belemnites ? Liversidgei, Eth. fil. 
 
 Ammonites inflatus, J. Sowerby, var. (Pl. 34, 
 ff. 1-4). 
 
 Ammonites Flindersit, McCoy (in well at 
 290 feet). 
 
 Ancyloceras Flindersi, McCoy (in well at 224 
 and 238 feet). 
 
 Crioceras, sp. ind. (Pl. 38, ff. 4-6—in well at 
 284 feet). 
 
 MUTTABURRA BORE. 
 
 PELECYPODA. 
 Inoceramus Crispii, Mantell ? 
 Paleomera ? sp. ind. (Pl. 26, f. 16). 
 
412 
 
 LIST OF FOSSILS FROM THE ROLLING DOWNS FORMATION IN 
 QUEENSLAN D—continued. 
 
 TOWER HILL. 
 (Landsborough River.) 
 CEPHALOPODA. 
 Hamites ? laqueus, Eth. fil. 
 
 ROCKWOOD STATION. 
 (Landsborough River.) 
 PELECYPODA. 
 Pecten, sp. ind. (Pl 21, f. 7 and 9). 
 Amusium, sp. ind. (Pl. 21, f. 4 and 4a). 
 Oxytoma rockwoodensis, Eth. fil. 
 Aucella hughendenensis, Eth. 
 
 LANDSBOROUGH RIVER. 
 (Five and a half miles north-north-west of 
 Rockwood Station.) 
 PELECYPODA. 
 Aucella hughendenensis, Eth. 
 
 JIRKING CREEK. 
 (Near Rockwood.) 
 PELECYPODA. 
 Aucella hughendenensis, Eth. 
 
 STONE HUT, ROCKWOOD CREEK. 
 PELECYPODA. 
 Aucella hughendenensis, Eth. 
 
 LANDSBOROUGH RIVER. 
 
 PELECYPODA. 
 Inoceramus Carsoni, McCoy. 
 Inoceramus marathonensis, Eth. 
 
 CEPHALOPODA. 
 Belemnites Canhami, Tate. 
 Ancyloceras Flindersi, McCoy. 
 Crioceras australe, Moore. 
 Crioceras, sp. ind. (Pl. 83, f. 4, 5, and 6). 
 
 REPTILIA. 
 
 Notochelone costata, Owen. 
 
 HEAD OF THOMPSON RIVER, BOWEN 
 DOWNS. 
 PELECYPODA. 
 Inoceranus. 
 WINTON. 
 PELECYPODA. 
 Unio (from Government well). 
 
 GYPSUM MINE, CHOLLARTON. 
 PELEOCYPODA. 
 Ostrea vesiculosa, J. Sowerby. 
 
 WARRIANA BORE. 
 (Twenty-five miles from Hughenden, on the 
 Winton Road.) 
 PELECYPODA. 
 Aucella hughendenensis, Eth. (at 351 feet). 
 CEPHALOPODA. 
 Ammonites inflatus, J. Sowerby (at 375 feet). 
 
 UPPER FLINDERS RIVER. - 
 PELECYPODA. 
 Cyprina Clarkei, Moore. 
 
 CEPHALOPODA. 
 Belemnites Sellheimi, Ten. Woods. 
 Belemnites Canhami, Tate (near Hughenden). 
 REPTILIA. 
 Ichthyosaurus australis, McCoy (Glendower 
 Station). 
 
 HUGHENDEN STATION. 
 PELECYPODA. 
 Aucella hughendenensis., Eth. 
 CEPHALOPODA. 
 Ammonites Flindersi, McCoy. 
 Ammonites Sutherlandi, Eth. 
 Ammonttes Daintreei, Eth. 
 
 PISCES. 
 Aspidorhynchus. 
 Belonostomus Sweeti, Eth. fil. and Smith 
 Woodward. 
 
 FLINDERS RIVER. 
 “(Seven miles above Marathon Station.) 
 
 InsrctA (NEUROPTERA). 
 Aeschna flindersensis, H. Woodward. 
 
 PELECYPODA. 
 
 Aucella hughendenensis, Eth. 
 Inoceramus pernoides, Eth. 
 
 MARATHON STATION. 
 (Flinders River.) 
 PELECYPODA. 
 
 Aucella hughendenensis, Eth. 
 Inoceramus Carsoni, McCoy. 
 Inoceramus pernoides, Eth. 
 Inoceramus marathonensis, Eth. 
 Inoceramus elongatus, Eth. 
 
 CEPHALOPODA. 
 Ammonites Sutherlandi, Eth. 
 
 REPTILIA. 
 Ichthyosaurus marathonensis, Eth. fil. 
 Plesiosaurus Sutherlandi, McCoy. 
 
 MAXWELTON. 
 (Flinders River.) 
 
 CEPHALOPODA. 
 Nautilus Hendersoni, With. fil. 
 
 BASE OF WALKER’S TABLE MOUNTAIN. 
 
 (Flinders River.) 
 
 PELECYPODA. 
 Inoceramus Carsoni, McCoy. 
 Inoceramus Sutherlandi, McCoy. 
 
LIST OF FOSSILS FROM THE ROLLING DOWNS FORMATION IN 
 QUEENSLAN D—continued. 
 
 BASE OF WALKER’S TABLE MOUNTAIN 
 
 —continued. 
 
 CEPHALOPODA. 
 Belemnites Canhami, Tate. 
 Ammonites Flindersi, McCoy. 
 Ammonites Sutherlandi, McCoy. 
 Aneyloceras Flindersi, McCoy. 
 
 REPriqia. 
 
 Ichthyosaurus australis, McCoy. 
 Plesiosaurus macrospondylus, McCoy. 
 Plesiosaurus Sutherlandi, McCoy. 
 
 FLINDERS RIVER, ON CAMBRIDGE 
 DOWNS RUN. 
 (Six miles from Richmond Downs Station.) 
 
 CEPHALOPODA. 
 Belemnites Canhami, Tate. 
 
 RICHMOND DOWNS. 
 (Flinders River.) 
 
 PISCES. 
 Lamna Daviesii, Eth. fil. 
 
 FLINDERS RIVER. 
 (Three miles above Richmond Downs Station.) 
 
 PELECYPODA. 
 Inoceramus Carsoni, McCoy. 
 Inoceramus Sutherlandi, McCoy. 
 
 FLINDERS RIVER. 
 
 (Thirteen and a half miles below Richmond 
 Station.) 
 
 PELECYPODA. 
 _ Inoceramus Carsoni, McCoy. 
 
 FLINDERS RIVER. 
 
 (Twenty-one miles below Richmond Downs 
 Station.) 
 
 PRELECYPODA. 
 Inoceramus Sutherlandi, McCoy. 
 
 FLINDERS RIVER. 
 (Thirty-five miles below Richmond Downs.) 
 REPTILIA. 
 Ichthyosaurus australis, McCoy. 
 NEAR MANFRED DOWNS. 
 (Flinders River.) 
 (Lat. 20° 5’ S., Long. 141° 43’ E.) 
 REPTILIA. 
 Ichthyosaurus australis, McCoy. 
 NEELIA CREEK. 
 (Near Cloncurry.) 
 
 PELECYPODA. 
 Aucella hughendenensis, Eth. 
 
 
 
 JULIA CREEK. 
 (Hughenden and Cloncurry Road.) 
 
 GASTEROPODA. 
 Natica Jackii, Eth. fil. 
 
 TATE RIVER. 
 
 CEPHALOPODA. 
 Crioceras australe, Moore. 
 
 WALSH RIVER. 
 PELECYPODA. 
 
 Pecten socialis, Moore. 
 Maccoyella Barklyi, Moore. 
 Pinna, sp. ind. (P1. 20, ff. 16 and 17). 
 Cyprina Clarkei, Moore. 
 Macrocallista ? plana, Moore. 
 Unicardium Meekii, Eth. fil. 
 
 CEPHALOPODA. 
 Belemnites Sellheimi, Ten. Woods. 
 Ammonites (Pl, 42, ff. 10 and 11). 
 Ancyloceras Taylori, Eth. fil. (head of River). 
 Crioceras australe, Moore. 
 Crioceras irregulare, Ten. Woods (head of 
 River). 
 ReEPTILIA. 
 Plesiosaurus. 
 
 PALMER RIVER. 
 
 PRELECYPODA. 
 Mytilus inflatus, Moore. 
 
 CEPHALOPODA. 
 Belemnites Sellheimi, Ten. Woods. 
 Ammonites olene, Ten. Woods. 
 Crioceras australe, Moore. 
 Crioceras irregulare, Ten. Woods. 
 
 KAMILAROI. 
 (Leichhardt River.) 
 PISCES. 
 Otodus appendiculatus, Agassiz. 
 LEICHHARDT RIVER. 
 (Seven miles from mouth of Gunpowder Creek.) 
 PELECYPODA. 
 
 Aucella hughendenensis, Eth. 
 
 INDEFINITE LOCALITIES IN THE 
 ROLLING DOWNS. 
 PELECYPODA. 
 Levicardium Brazieri, Eth. fil. 
 
414: 
 
 The above List of Fossils has enabled my Colleague to refer the Rolling Downs 
 Formation to the Cretaceous; although he admits that the formation contains “an 
 admixture of Oolitic as well as Cretaceous life.” As the succeeding formation (the 
 Desert Sandstone) is, although it rests unconformably on the Rolling Downs, also 
 recognised as Cretaceous, we class the Rolling Downs and Desert Sandstone respectively 
 as Lower and Upper Divisions of that Period. 
 
 The break between the Rolling Downs and the underlying Ipswich Formation is 
 complete so far as regards its life-history. The only fossils they have m common are 
 two species of Unio in each, but they are not the same species, and, even if they were, 
 the presence of such a widely distributed form would have little significance. 
 
 With the succeeding formatiou, the Desert Sandstone, although separated from 
 it by a violent unconformability, the elias Downs appears to have more in common, 
 unless, indeed, the early collectors, who did not suspect that there was any distinction, 
 mixed up fossils from the two formations as developed in the neighbourhood of 
 Wollumbilla and Mount Abundance. With this reservation, we recognise as common 
 to the two formations the genera Rhynchonella, Ostrea, Lima, Pseudavicula, Maccoyella, 
 Cucullea, Nucula, Tr igonia, Cyprina, Paleomera, Glycimeris, Pecten, Natica, and 
 Belemnites ; and the species Maccoyella Barklyi, M. reflecta, M.? wmbonalis, AM. ? 
 corbiensis, M.? substriata, Cyprina Clarkei, Glycimeris rugosa, Ni wcula quadrata, and 
 Natica variabilis. 
 
 ARTESIAN WELLS. 
 
 The Western Interior of the Colony, especially that part’ which is covered by the 
 Rolling Downs Formation, is covered with rich grasses, but in dry seasons the greater 
 portion of the grass ceases to be available for stock, owing to the distance from water. 
 For many years the Government and the pastoral lessees of the Crown laboured to 
 counteract this disadvantage by excavating tanks and throwing dams across water- 
 courses for the conservation of water. The enormous expense of these undertakings, 
 however, prevented the general adoption of this method of meeting the difficulty. In 
 many cases, besides, the soil proved unsuitable for the retention of water ; and in some 
 instances I believe that the rainfall is so slight that, if the whole of it could have been 
 conserved in the districts where it fell, it would not have sufficed to render the herbage 
 available. 
 
 The great drought which prevailed in the year 1885 brought about a feeling akin 
 to desperation, and I was sent along with Mr. J. B. Henderson, Hydraulic Engineer, 
 with instructions to study the structure of the Western Country, and report whether 
 there was a chance of success in boring for artesian water, and if so, to determine the site of 
 the first experiment. I came to the conclusion that the conditions were similar all over the 
 Western Downs; that the strata of the “ Rolling Downs Formation ”’ cropped out on the 
 flanks of the eastern ranges, and dipped westward under the plains, with undulations 
 regarding which we had, and could have, no data, so that it was impossible to predict at 
 what depth water might be struck in any individual case. In these circumstances we 
 recommended that the first bore should be made at Blackall, which appeared at the time 
 to be in the sorest need. 
 
 The bore at Blackall proved successful, although, owing to an accident, it was not 
 the first to strike artesian water, the Barcaldine Bore having carried off that honour. 
 Since then boring for artesian water has been carried on vigorously all over the 
 Western Interior, and a week seldom passes without information reaching me of the 
 success of some fresh bore. : 
 
 Operations were carried on at first with the Pennsylvania Beam-Borer, and latterly 
 with the Canadian Pole-Borer. These instruments carry on the work rapidly, and at a 
 
415 
 
 comparatively small expense. But in one important particular they fall short of the 
 requirements of a perfect boring tool. It is impossible to obtain a record of the strata 
 cut through. Had such a record been obtained, and systematically preserved, there 
 must have been by this time an accumulation of data invaluable for the purpose of 
 directing and economising future operations. Owing to the manner in which the 
 material is pounded up, the strata of one bore can never be “read” with those of 
 another. All that it is open to us to record is the depth at which artesian water has 
 been met with in various localities, and with this, for the present, we must rest content. 
 I append to this Chapter, for reference, such records as have reached me on the subject. 
 
 From this record it will be observed that in some cases artesian water has been 
 met with at comparatively shallow depths in the vicinity of springs, and for the most 
 part in the vicinity of thermal springs. The subjects of artesian water and thermal 
 springs have evidently an intimate connection. 
 
 To begin with thermal springs, the first thing we discover is how extremely vague 
 and unsatisfactory are the explanations offered by the best authorities. The whole of the 
 light hitherto thrown on the subject may be summed up in the following quotation from 
 Dr. A. C. Peale’s Report on the Thermal Springs of the Yellowstone National Park * :— 
 “Everywhere that observations have been made, there appears to be an increase (of 
 temperature) as we descend towards the centre of the earth. In this increase of heat, 
 of course, we have sufficient reason for the heat of springs coming from a great depth. 
 In many thermal springs, however, as in our Yellowstone Region, this regular increase 
 in temperature is not sufficient to account for the high temperature, and we must look 
 for the cause in plications and faults or in the voleanic rocks in which the springs are 
 located.” 
 
 Rocks of igneous origin (e.g., basalts) may, and in some cases must, still retain 
 at comparatively shallow depths enough of their original heat to raise the temperature 
 of any water with which they may come in contact to what is usually understood by the 
 boiling-point—z.e., the boiling-point under the pressure of one atmosphere. But the 
 contact must take place at depths so shallow that the pressure of suprajacent water or 
 rock shall not raise the boiling-point of water above the temperature of the rock. 
 Every lava-flow which appears at the surface must be connected with underground 
 ramifications, consisting essentially of a “reservoir” and a channel. The material in 
 both reservoir and channel must, at least in the case of all but very recent eruptions, 
 be consolidated ; but rocks of the lava class are very bad conductors of heat, or, in other 
 words, part with their original heat very slowly. The connection of hot springs in all 
 parts of the world with recent or, geologically speaking, not very ancient volcanic rocks, is 
 now well known. 
 
 Careful observations have shown that, so far as the investigations could be 
 carried, the internal heat of the Earth increases about 1° Fahrenheit for every fifty or 
 sixty feet of depth, and it might be thought that, from this cause alone, wherever water 
 could penetrate to sufficient depth it would be boiling, but this can easily be shown to 
 be an error. Assuming an increase of one degree in fifty feet, and the surface tem- 
 perature to be seventy degrees, a depth of at least seven thousand one hundred feet 
 would have to be attained before the rock forming that portion of the earth’s crust, or 
 water in contact with it, would have a temperature of 212°. Nevertheless, a column of 
 water reaching from the surface to a depth of seven thousand one hundred feet would 
 not by any means have its base at the boiling-point, because the boiling-point of water 
 is raised enormously by pressure. From observations made at the Great Iceland 
 
 * Twelfth Ann, Report U.S, Geol. Geogr, Survey of the Territories for 1878, Pt, 2, Washington,1883, 
 
416 
 
 Geyser it was found that the boiling-point rose from 210° at the surface, to 278° at the 
 depth of seventy-seven feet. This ratio, giving a rise of the boiling-point of 68° 
 in seventy-seven feet, would make the boiling-point of water at seven thousand one 
 hundred feet not 212°, but 6,366° (and that merely under the pressure of a column 
 of water, while the pressure of a column of rock would be about two and a-half 
 times as much). These astonishing figures prove that the ratio of the rise in the 
 boiling-point being higher than the ratio of the increase of the earth's temperature 
 with depth, water would never be raised to boiling-point by the internal heat of the earth 
 alone. 
 
 At the same time, though water would not boil from the internal heat of the 
 earth, yet where it exists beneath seven thousand one hundred feet it must always 
 have a temperature above 212°. Immediately upon the production of an outlet, 
 whether by natural means, such as a fault or earthquake fissure, or by artificial means, 
 such as a bore, the relief of pressure would bring about a rise of the water in the fault, 
 fissure, or borehole analogous to that of the rise of the mercury in the tube of a 
 thermometer. 
 
 In the case of athermal spring it is not necessary that the fissure should be open 
 down to a depth of seven thousand one hundred feet, asthe requisite high temperature 
 may be found when the water is in contact with subterraneous igneous rocks still 
 retaining much of their original heat. 
 
 In the artesian wells of our Western Interior, the water issues at temperatures 
 which are high, although still far below boiling-point—e.g., Back Creek 70°, Aramac 
 Private Bore No. 1, 81°, Muckadilla 124°, Barcaldine 102°, Saltern Creek Government 
 Bore 115°, Saltern Creek Private Bore No. 8, 128°, Blackall 119°, Tambo 98°, Cunna- 
 mulla 106°, Charleville 106°, Manfred Downs No. 2, 110°, No. 10, 118°. 
 
 There are, as already mentioned, few records of the strata passed through, but at 
 all events there is nothing to show that any igneous rocks whatever have been met with 
 in the bores. The high temperature of the water may be taken to be the result solely 
 of the internal heat of the earth. It will, however, be observed that the temperature 
 of the water does not bear a constant relation to the depth. The internal heat must, 
 therefore, have affected the temperature of the water elsewhere than in the places 
 where the water has been tapped. 
 
 Now, although the temperature of the water of the artesian wells is somewhat 
 high, the depth at which it has been struck is in no case great enough to account for tt. 
 For example, the temperature of 119° attained at 1,663 feet in the Blackall Bore 
 would not be reached by the rock before the bore had been carried to the depth of 2,450 
 feet, assuming that the constant surface temperature is 70°, and the increase with depth 
 one degree in fifty feet. The water, I take it, must have reached, with the undulations 
 of the permeable strata containing it, lower depths than those at which it has been tapped 
 by the bores. This is to my mind a confirmation of the view I have always held, that the 
 Rolling Downs strata undulate considerably. 
 
 The commonly accepted theory of. artesian wells is that a permeable stratum, 
 with impermeable strata both above and below, carries water from its outcrop down to 
 whatever depth it may be buried beneath accumulations of later date, and that on tapping 
 the water-charged stratum the water will rise to, or near, the level of the outcrop of the 
 stratum. ‘Till lately I have rigorously adhered to this theory, which perfectly accounts 
 for many of the best-known artesian wells of Europe and America, but in the case of 
 the Queensland wells it is doubtful if the strata in which the water has been tapped 
 crop out at elevations sufficient to give the pressure required to raise the water to the 
 surface. 
 
417 
 
 It is indeed difficult to identify the outcrops of the strata in which the water has 
 been tapped, but at allevents they cannot be at higher levels than theline where the 
 edgeof the Rolling Downs Formation meets the Paleozoic rocks on which the formation 
 rests. The difficulty of the case is increased by the fact that the Rolling Downs Forma- 
 tion is generally overlapped by the Desert Sandstone Formation, so as to obscure its 
 junction with the Paleozoic rocks. It is probable that the outcrops of the permeable 
 strata are seldom more than five hundred feet above the level of the surface of the 
 ground in the places where the permeable strata have been tapped, with the result of 
 finding overflowing artesian water. 
 
 Mr. J. Hugh Moor, Manager of Manfred Downs Station, on the Flinders, has 
 courteously forwarded to me samples of the rock in which the water from his “ No. 2 
 Well” was struck. A more favourable medium for the conveyance of water could 
 scarcely be imagined. It is a sandstone so open that water can be sucked through it as 
 easily as through a piece of spongy iron. But even if, instead of a stone filter (however 
 open), the water had to pass through an iron pipe, there would still be such a loss by fric- 
 tion in two or three hundred miles, that it could not rise quite to the level of its source. 
 
 My belief is that the water flowing from an elevated source down the plane of a 
 permeable stratum intercalated between two impermeable strata must rise, in a bore 
 tapping the permeable stratum, to near the level of its source, and be aided in its rise 
 by expansion due to heat acquired in its passage over a portion of the stratum now 
 lying at a lower level than that at which it was tapped by the bore. 
 
 The Desert Sandstone, which, where not denuded, always rests on the Rolling 
 Downs Formation at high levels, and unconformably, is itself a great reservoir of water, 
 which issues in springs from the cliffs at the edges of the table-lands which are its 
 characteristic feature. Some of the water with which the Desert Sandstone is charged 
 must find its way into any permeable beds in the Rolling Downs Formation whose 
 outcrop may happen to be covered by the Desert Sandstone. 
 
 The expansion of the water itself would probably be greatly assisted by the elasticity 
 of imprisoned gases increasing in volume in proportion as they are relieved of pressure. 
 
 Tt has been suggested that the pressure of water implied by Australian artesian 
 wells may be derived from strata in the mountains of New Guinea, or even of the 
 Himalayas. It must be recollected, however, that only open and porous strata can 
 possibly act as conduits for water, and that strata of this character (gravels, conglomerates, 
 grits, and sandstones) are necessarily local in their distribution, as they could not 
 possibly be deposited in a deep sea far from the land. It is within the bounds of 
 possibility, seeing how little we know of New Guinea, that the Rolling Downs 
 Formation may extend across the strait separating Queensland and New Guinea, and 
 that the “head of water’’ may be derived from the latter island, as we know at least that 
 Cretaceous rocks occur in New Guinea.* From what has already been said as to the 
 non-continuity of open and permeable strata across oceanic depths, it is, however, to 
 say the least, highly improbable. As regards the continuity of Cretaceous rocks of the 
 Rolling Downs age from Queensland to India, the idea is too extravagant to be enter- 
 tained for a moment by any Geologist. 
 
 Considering the paramount importance of the question of artesian water in the 
 West, I have thought it well to record briefly in the following pages such particulars as 
 I have been able to ascertain regarding the wells already sunk. For a great deal of this 
 information Iam indebted to Mr. J. B. Henderson, M.I.C.E., Government Hydraulic 
 Engineer. 
 
 * From the recent information collected by Mr, A. Gibb Maitland (see Chapter on British New 
 Guinea), it must be admitted that this is hardly possible, 2 
 2c 
 
 
 
 
 
418 
 
 It is a well-known fact that in California, the London Basin, and many other 
 localities where artesian wells are numerous, the overflow has diminished, and in some 
 cases altogether stopped. For the sake of argument I have summed up the amount 
 which would overflow from a// the Queersland bores mentioned in the following pages 
 if they were allowed to run without check. The total amounts to 58,177,760 gallons 
 per day, or 21,234,882,400 gallons per annum, which is equal to the total annual rainfall 
 over nearly seventy-two square miles, taking it at an average of 20°45 inches.* Granting 
 that the rainfall is greater in the coastal regions where the water-bearing strata may 
 be supposed to crop out, what may be called the expenditure still bears an alarmingly 
 large proportion to what may be called the income, for it must not be forgotten that 
 the length of the outer boundary line of the Lower Cretaceous Formation is the maximum 
 possible length of the outcrop of any water-bearing or other stratum init. Even athick 
 water-bearing stratum would only occupy with its outcrop a breadth of a few chains at most; 
 so that it would take many miles 77 length of the outcrop of such a stratum to receive 
 that portion of the rainfall of a square mile which is not carried off by streams or 
 evaporated. It may; therefore, be safely predicted that if artesian wells become much 
 more numerous, and if all be allowed to overflow, a diminution of the supply may shortly 
 be looked for. It is gratifying that the Government is taking steps to prevent 
 the waste of artesian water. It seems to me that the use of the water should be 
 restricted to stock-watering and town supply. Even irrigation I should regard as wilful 
 waste, unless indeed, after the lapse of years, there should be found to be no diminution 
 
 in the supply. 
 
 PARTICULARS OF BORES IN THE ROLLING DOWNS. 
 ROCKLANDS. 
 
 A bore at Rocklands Station, on Pring Creek, a tributary of the Georgina River, 
 _ in the Barkly Table-land, still, I believe, incomplete, shows several alternations of strata, 
 including, as I read it, not only Lower Cretaceous strata, but also the Desert Sandstone, 
 some Tertiary rocks, and overlying basalts. 
 
 The site of the bore is about six hundred feet above sea-level, and about Lat. 
 19 40’, and Long. 188° 15’. The section has been kindly handed to me by Mr. A. 
 
 Rourke : ~ 
 
 Feet. 
 
 Hardened clay and boulders Fe on fe e373) 
 
 siete ee clay sé a os see os oe oe 
 Rotten limestone is ig ae Ke 7 mE 3 
 
 [Rosin limestone with basalt seams nae nae rele 
 
 Basalt + Basalt and lime rock... Bee 4 3 rae SS aa Gt 
 ims rock op os a) ies ote Bee es) 
 
 Basalt .., se at ae = Se ot Pre eed' | 
 
 Lime rock HAs saa ae a oe ace aay ye 
 
 Red sand bee is a ah ae a Be at 
 
 Lime, iron, and sandstone .., i ie eas oh ali 
 
 Rotten limestone and red clay are a = te eed 
 
 Rotten rock and boulders... ot * + oeeLG 
 
 Tertiary ? < Porous lime rock with flinty seams e AS “eg 
 Hard lime rock se ae er bee an ae 
 
 Rotten porous limestone cet mae 5a Fel) 
 
 \ Hard lime rock ~~ Sei ie ae ase Pom 
 \ Rotten rock ... ce oa <? “i + fcr ts) 
 Lime rock “10 an se a ae a sceele 
 
 
 
 
 
 * This is the average rainfall at Charleville for the eleven years ending with 1890, 
 
419 
 
 Feet. 
 
 = 
 oe 
 
 Hard flinty rock 
 White sand 
 White sand rock 
 Flinty lime... ee sty ae 
 Flinty lime, shattered, with crevices 
 ; Flinty lime rock ¥ 
 White sand— Water ... 
 Desert Sand- j Shattered white sand rock 
 stone P Flinty, hard sand rock } 
 White sand rock ee 
 Hard compact sand rock 
 White sand rock— Water * ... 
 Flint ae ate 
 Sand rock Ae es 
 Flint rz ace ne 
 Brown sand (August 1, 1890) 
 Sand rock with seams of limestone... 
 Pure limestone 
 Cretaceous ? | Gaver a7 a. a se sie 4 
 Yellow ochre and black sand with stones ... 
 
 Pitan rock ,., a AY) 
 
 bo 
 
 a 
 AATOORMWNOCANUNABRNWAD Ww 
 
 
 
 Oo) 
 
 12 
 WARRENDA.—Lat., 22° 45’, Long. 140° 55’. i 
 
 Several private artesian wells have been sunk on this Run, yielding large 
 supplies of water from shallow depths. The deepest (No. 5) is seven hundred and 
 fifteen feet, and supplies 750,000 gallons per day. It is stated that several mud 
 springs break out in this neighbourhood between the different channels of the Hamil- 
 ton River. It may be noted that Warrenda New Station is not in the position shown 
 on the map (which is the site of the Old Station), but about sixty miles higher up 
 the river. The deep bore above referred to is on Polygammon Creek, No. 4 Bore is 
 five hundred and eleven feet deep, and supplies 150,000 gallons per day. No. 2 Bore is 
 one hundred and eighty-four feet deep, and supplies 70,000 gallons per day.t 
 
 No. 6 Bore. Supply, 1,000,000 gallons per day. Depth, seven hundred feet. § 
 Water struck at five hundred and fifty feet.|| 
 
 No. 7 Bore. Depth, seven hundred and seventy-three feet. Water overflowing 
 at the rate of 400,000 gallons per day.{ 
 
 » MAXWELLTON, No. 1 BORE, 
 Water overflowing at the rate of 300,000 gallons per day. Depth not stated.** 
 
 AVON DOWNS.—Lat. 20°, Long. 137° 30’. 
 A bore has been sunk on this Station, which is situated on Rankin’s Creek, 
 Georgina River (on the South Australian side of the border), at a height of about 
 five hundred and fifty-four feet above sea-level. "Water was struck at two hundred feet 
 but did not flow over the surface. 
 
 
 
 
 
 * Rose to 275-feet level. No mud, though there was a current. 
 
 + Approximate latitudes and longitudes are given throughout for the purpose of enabling the reader 
 to locate the bores on the map. 
 
 t{ Hydraulic Engineer’s Report on Water Supply for Year ending 30th June, 1891, Brisbane: by 
 Authority : 1891, And information furnished by Mr. G, Neville Griffiths, 
 
 § Brisbane Courier, 4th September, 1891, 
 
 || Ibid., 25th January, 1892. 
 
 {| Ibid., 26th March, 1892. 
 
 ** Tbid., 10th February, 1892, 
 
420 
 
 MANFRED DOWNS (Private).—Lat. 20° 8’, Long. 141° 40. 
 
 No. 1 Bore. 
 Clay ey a ft ae ate aa mh Ane ra ... 60 feet 
 Blue shale Hts ae ee ar $8 a ia ae con YAO 
 tide ee nett ay 
 
 Water-bearing sandstone ‘ 
 The water rises six feet above thal ntact in a one- ahee pipe at the rate of 50,000 
 
 gallons per day.* 
 
 No. 2 Bore. 
 Blue shale to... so: or a He a iH =a .. 665 feet 
 Shale and sandstone to me + ae ya hee 
 Hard fine-grained porous sandstone: ati water af in 3° at : ZO Re 
 a 33.) 60 mee 
 
 Softer and coarser sandstone with water at 
 The water flows over the surface at the rate of 526 ,000 gallons per day, with a 
 
 temperature of 110° F.+ 
 In a table attached to the Hydraulic Engineer's Annual Report, 30th June, 1891, 
 
 the following additional information is given regarding bores at Manfred Downs :— 
 
 No. Depth in Feet. Supply per diem. — ’ Temperature. 
 Gallons. 
 
 1 ity 22,000 Overflowing. 
 
 2 128 12,000 op 
 
 3 86 14,000 rf 
 
 4 210 10,000 5p 
 
 5 200 20,000 Not overflowing; supply pumped. 
 
 6 98 16,000 Overflowing. 
 ah 678 50,000 4 see sac aie 68 106° 
 ts 760 525,000 dee oe oti me 110° 
 
 9 "07 200,000 2 SE ell D 6 td 5 102° 
 10 733 250,000 | ny aes nib ose see 118° 
 
 
 
 RICHMOND DOWNS, Flinders River (Private).—Lat. 20° 45’, Long. 143° 10’. 
 
 There are five bores on this Station. No. 1 Bore is six hundred and ninety-eight 
 feet deep. Water flows over the surface at the rate of 1,600,000 gallons per day.§ 
 Temp., 96°.|| No.2 Bore is situated on Alexandra Creek, on the north side of the 
 Flinders. At four hundred feet a supply, estimated at 1,000,000 gallons per-day, was 
 struck. The Newspaper Correspondent, in announcing the discovery, mentions that the 
 bore was put down in eight days, and adds that “the water is splendid, and equal to if 
 not better than that in the last bore.”“ Total depth, four hundred and eighty feet ; 
 yield, 1,200,000 gallons per day; temperature, 92°.|| 
 
 No. 4 Bore tapped a supply of water at a depth of six hundred feet, yielding 
 2,000,000 gallons per day.** 
 
 No. 5 (?) Bore. Depth six hundred feet; water overflowing at the rate of 
 2,000,000 gallons per day. ‘‘The result of the present bore brings the total supply for 
 the five bores at less than 1,000 feet each, to 8,000,000 gallons per day.’’++ 
 
 * Letter from Mr. J. Hugh Moor, 1st January, 1889. 
 
 + Ibid., 12th December, 1889, 
 
 ~ Nos. 7 and 8 are evidently the bores named Nos. 1 and 2 respectively in Mr. Moor’s letters. 
 § Townsville Bulletin, 26th June, 1891. 
 
 || Hydraulic Engineer’s Report, 30th June, 1891. 
 
 {| Townsville Bulletin, 23rd July, 1891. 
 
 ** Brisbane Courier, 11th November, 1891. 
 
 tt Brisbane Telegraph, 9th November, 1891, 
 
491 
 
 MARATHON, No. 1 BORE. 
 Water overflowing at the rate of 2,300,000 gallons per day; depth not stated.* 
 
 MACKINLAY BORE, on the Mackinlay River (Government).—Lat, 21° 25’, Long. 141° 26’. 
 
 When at the depth of cight hundred and thirty-seven feet, water rose over the 
 surface at the rate of 160,000 gallons per day. Total depth, 1,002 feet ; overflow, 
 350,000 gallons per day. The bore pierced the following strata :—“ Alluvial layer; 
 yellow clays; blue and grey shales, irregularly interstratified with thin beds of grey 
 and brown sandstone, now and then of a slightly greenish tint; and calcareous seams. 
 Occasionally mundic was brought up in the sand pump. The water was tapped in 
 coarse open sandstone.” f 
 
 TOORAK, No. 2 BORE, Mackinlay River (Private). 
 
 Depth, 1,550 feet; water overflowing at the rate of about 1,000,000 gallons 
 
 per day.t 
 STRATHFIELD STATION, Mackinlay River, Burke District (Private . 
 
 Depth, eight hundred and thirty feet; water flowing at the rate of 500,000 
 gallons per day.§ 
 
 WERNA.—Lat. 21° 50’, Long. 143°. 
 
 Water was struck in a well on the boundary of Werna and Ayrshire Downs Runs 
 at one hundred and forty feet, and again at one hundred and eighty feet. The water 
 rose seventy feet in the well; at least it stood at one hundred and thirty-four feet from 
 the surface in December, 1881, when I visited the place after a protracted drought. 
 The section met with in this well has already been described (p 402). 
 
 SHEPPARD’S WELL, Winton.—Lat. 22° 22’, Long. 148° 3’. 
 No water was met with in this well, which was sunk to the depth of one 
 hundred and thirty-five and a-half feet. The strata met with have already been 
 
 described (p. 402). 
 GOVERNMENT WELL, Winton (behind Court House). 
 
 No water at one hundred and fifty feet. The strata have already been described 
 (p. 403). 
 
 WINTON BORE (Government), 
 
 Depth, at 30th June, 1891, 1,800 feet. 
 
 Strata :— An alluvial layer; sandy shale, soft and indurated fine-grained grey 
 shales, occasionally of a slightly greenish tint, and bluish-coloured sandstones, irregularly 
 interstratified. One or two thin beds of what appeared to be carbonaceous shales, and 
 some dark material, evidently coal, were passed through. . Several small samples of 
 gypsum were brought up by the sand pump.” At 1,260 feet, a small stream of water 
 was struck, which rose to within about fifty feet from the surface. 
 
 : VINDEX, near Winton,—Lat. 22° 28’, Long, 143° 19’, 
 In a well at the Station, water was struck, about 1880, at one hundred and 
 ten feet, and rose twenty-five feet. The strata have already been described (p. 403). 
 
 * Rockhampton Bulletin, December, 1891. 
 
 + Hydraulic Engineer’s Report, 30th June, 1891. 
 + Brisbane Courier, 16th March, 1892, 
 
 § Ibid., 27th October, 1891, 
 
422 
 
 A second well was sunk at Crawford’s Creek, nine miles east of Vindex, and 
 water was obtained at one hundred and fifty feet. The strata have already been 
 described (p. 403). 
 
 A bore was sunk on Vindex Run, about seven miles N. 15° E. of the Station, but 
 at the depth of one hundred and eighty-seven feet had not struck water. The strata 
 have already been described (p. 403). 
 
 MANUKA.—Lat. 21° 45’, Long. 143° 25’. 
 
 On Manuka Station two wells were sunk prior to 1881. The first, close to the 
 Station, struck water at eighty feet. More came in at one hundred and two feet. At 
 one hundred and forty feet a large supply came in, making about thirty-six feet of 
 water in twenty-four hours, and a few days later seventy feet of water stood in the 
 shaft. The water was rather brackish, but cattle drank it readily. In the second well 
 a little water came in at one hundred feet. More was found at one hundred and thirty 
 feet, and the quantity increased till at one hundred and eighty feet a large supply was 
 struck. The water stood seventy-seven feet deep, and was less brackish than that of 
 the first well. The strata passed through in both wells were grey flags or shales, with 
 bands of bluish sandstone, containing indistinct plant-remains and a few shells. The 
 specimens of the latter, preserved by Mr. Anderson, of Manuka, had fallen to pieces on 
 exposure to the air, and nothing remained of them but fragments. 
 
 BOWEN DOWNS BORES (Private).—Lat. 22° 30’, Long. 145°. 
 No.1, Depth, nine hundred and seventy feet; overflow, 493,600 gallons per 
 day ; temperature, 90°; pressure per square inch, 70 Ib. 
 No. 2.* Depth, 1,374 feet; overflow, 1,500,000 gallons per day; temperature, 
 103°. 
 No. 3. Depth, 1,112 feet; overflow, 864,000 gallons per day.+ 
 
 COREENA BORES, near Aramac (Private).—Lat,. 23° 25’, Long. 145° 25’. 
 
 On this Run there are three bores, A, B, and C, which have tapped an over- 
 flowing supply, and four (D, E, F, and G) which have struck water which rises but does 
 not overflow. 
 
 Bore A is nine hundred and four feet deep ; overflow, 1,500,000 gallons per day. 
 
 Bore B is 1,350 feet deep; overflow, 350,000 gallons per day. 
 
 Bore C {is 1,100 feet deep; overflow, 150,000 gallons per day. 
 
 Bore D, at two hundred and eighty-five feet, and Bore E, at four hundred and 
 fifty feet, tapped small supplies of water which did not overflow. 
 
 Bore F, at seven hundred and fifty feet, struck a supply which rose at first to 
 forty feet, and afterwards to twelve feet from the surface, and from which 40,000 
 gallons per day can be pumped. 
 
 Bore G. Depth, three hundred feet; water rises to within four feet of the 
 surface ; 25,000 gallons per day can be pumped. 
 
 CORINDA BORE, near Aramac (Private).—Lat. 22° 40’, Long. 145° 40’. 
 Depth, five hundred feet. Water flowing over surface at the rate of 150,000 
 gallons per day.§ 
 
 * In middle of ‘‘ Herbert” Block. 
 
 + Hydraulic Engineer’s Report, 30th June, 1891. 
 
 t+ Known as DaJzell’s Bore, Newark Block, Coreena, 
 § Townsville Bulletin, 7th June, 1890, 
 
423 
 
 SALTERN CREEK BORES (Private).—Lat. 23° 30’, Long. 144° 50’. 
 
 Bore No.1. Depth, 1,180 feet ; water overflows at the rate of 175,000 gallons 
 per day ; temperature, 108°.* 
 
 No. 2. Depth, 1,605 feet; water overflows at the rate of 220,C00 gallons per 
 day ; temperature, 113°; pressure, 31 1b. per square inch.* 
 
 No. 3. Depth, 1,970 feet ; water overflows at the rate of 690,000 gallons per 
 day ; temperature, 128°; pressure, 491b. to the square inch.* 
 
 No. 4. Depth, 1,560 feet ; water overflows at the rate of 1,000,000 gallons per 
 day. 
 
 SALTERN CREEK BORE (Government). 
 
 Depth, nine hundred and seventy-eight feet; water overflows at the rate of 
 
 17,200 gallons per day; temperature, 115°; pressure, 88 Ib. to the square inch.* 
 
 ANALYSIS OF THE WATER BY R. Mar, GoveRNMENT ANALYST. 
 
 Total fixed salts... She san 5p tte ae 6c PLOoIDU 
 Carbonate of calcium aie ats an re er ee seer Ot 
 
 A » Magnesium ... ‘ ee ise .. trace 
 Chlorides and carbonates of pants ad hep oee ec eve we 81°42 
 Oxide of iron 5 at ae wee one .» L'04 
 
 Unfit for sake May be used for other purposes. 
 
 BARCALDINE BORE (Government).—Lat. 23° 30’, Long. 145° 10’, 
 
 Site nine hundred and fifty-three feet above sea-level; depth of bore, six hundred 
 and ninety-one feet nine inches; water rises twelve feet four inches above surface in a 
 ten-inch pipe at the rate of 175,000 gallons per day ; temperature, 102°; pressure, 17 lb. 
 to the square inch; cost of bore, £775. 
 
 In his next Annual Report, Mr. Henderson notes: ‘‘ This bore has maintained its 
 reputation for yielding a large supply of excellent fresh water. Nothing has been done 
 since the date of my last report to enable the Department to shut off with safety the 
 flow of the water, by means of the screw-plug and valve with which the casing is 
 furnished.” Thrown open for bathing purposes with beneficial effects.* 
 
 ANALYSES OF WATER BY R. Mar, GOVERNMENT ANALYST. 
 
 First. Second, 
 Total fixed salts ... eae ... 66°50 se 63°70 
 Organic matter ... “oe ... trace ae trace. 
 Chlorine... ied tee ... small quantity abe small quantity. 
 Sulphuric acid .., 7 ... trace ae trace. 
 Ammonia ... se aes ... trace ae trace. 
 Albuminoid ammonia... ... slight trace slight trace. 
 
 Hardness, 2° 8’. The salts in solution are chiefly bicarbonates ime sodium and potassium. There- 
 fore, while the water may be used for domestic purposes, they are unfit for use in irrigation. 
 
 BACK CREEK BORE, east of Barcaldine.—Lat. 23° 35’, Long. 145° 45’, 
 
 This bore, sunk for the Railway Department, struck, at the depth of one hundred 
 and eighty feet, water which overflows at the rate of 72,000 gallons per day, with a 
 temperature of 70° and a pressure of 5 |b. to the square inch. 
 
 * Hydraulic Engineer’s Report, 30th June, 1891. 
 + Brisbane Courier, 18th March, 1892. 
 + Hydraulic Engineer’s Report, 30th June, 1889, 
 
424 
 
 FRASER’S SELECTION BORE, seven miles North of Barcaldine (Private).—Lat, 23° 23’, Long. 145° 10’. 
 Depth, 1,175 feet; overflow, 600,000 gallons per day. 
 
 FRASER AND McLACHLAN’S BORE, near last (Private). 
 Depth, seven hundred feet ; overflow, 200,000 gallons per day. 
 
 TARA BORE, twenty miles West of Barcaldine (Private).—Lat. 23° 30’, Long. 144° 35’. 
 Depth, 2,003 feet ; overflow, 250,000 gallons per day. 
 
 BARCALDINE WELL (Private). 
 
 I have been informed by Mr. J. V. 8S. Desgrand that a well at Barcaldine Station, 
 one hundred feet deep, struck salt water; as did also a well on the Barcaldine Run, on 
 
 the eastern side of the Alice. 
 
 DARR RIVER DOWNS BORES (Private).—Lat. 23°, Long. 144°. 
 Bore No. 1. Depth, 2,007 feet; brackish water rose to seventy feet from 
 surface; temperature, 107°; 20,000 gallons per day can be pumped. 
 Bore No. 2. Depth, 1,007 feet ; 40,000 gallons per day can be pumped. 
 Bore No. 3. Depth, 2,700 feet ; overflow, 50,000 gallons per day. 
 Bore No. 4. Depth, 800 feet; 4,800 gallons per day can be pumped.” 
 
 ALICE DOWNS BORE (Private).—Lat. 24° 10’, Long. 145° 30’. 
 Depth, 2,145 feet ; overflow, 100,000 gallons per day.* 
 
 EVORA BORE (Private).—Lat. 24° 15’, Long. 145° 30’. 
 Depth, 2,036 feet ; overflow, 43,000 gallons per day ; temperature, 116°. 
 
 HOME CREEK BORE (Private).—Lat. 23° 55’, Long. 145° 20’. 
 
 From a bore, 1,760 feet deep, water overflows at the rate of 100,000 gallons 
 daily.* 
 
 " BLACKALL BORE (Government).—Lat. 24° 25’, Long. 145° 30’. 
 
 Depth, 1,663 feet ; water overflows at the rate of 300,000 gallons per day; 
 temperature, 119°; pressure, 65 Ib. to the square inch.* In his ‘Annual Report,” 30th 
 June, 1890, Mr. Henderson has the following note :—“ This work is in good order, and, 
 so far as I am aware, the discharge and pressure of the water have not diminished. 
 The flow of water from this bore, like that from all the others, save Barcaldine, can be 
 completely shut off and otherwise controlled at pleasure.” 
 
 ANALYsSIs OF WATER BY R. Mar, GOVERNMENT ANALYST. 
 
 Total fixed salts... sn oy te aes aes ~, 71°40 
 
 Organic matter... sare a a5 rs we see | DTECO, 
 Chlorine... hy aa 3 ay i ae ... Small quantity. 
 Sulphurie acid... as ane ae fe ns ... ‘Trace. 
 Ammonia ... ae me dee if ss afb aa race, 
 Albuminoid ammonia... Slight trace. 
 
 Hardness, 3°, The salts in solution are chiefly bicarbonates of sodium and potassium. There- 
 fore, while the waters may be used for domestic purposes, they are unfit for use in irrigation.* 
 
 The unsuccessful “Town Well’ at Blackall, two hundred and fifty feet deep, 
 gave a section of a portion of the strata probably similar to those met with in the bore 
 (see page 405). 
 
 WESTLANDS BORE (Private).—Lat. 23° 55’, Long. 148° 48’. 
 
 Depth, 2,036 feet ; no overflowing water. 
 
 * Hydraulic Engineer’s Report, 30th June, 1891. 
 
425 
 
 TAMBO BORE (Government).—Lat. 24° 50’, Long. 146° 15’. 
 
 Depth, 1,002 feet ; water overflows at the rate of 200,000 gallons per day; tem- 
 perature, 98°; pressure, 12 lb. to the square inch.* In his report Mr. Henderson states : 
 “On 10th September [1888] good water was tapped in sandstone, and a larger supply of 
 excellent fresh water was struck at nine hundred and ten feet; at 1,002 feet drilling 
 was stopped. An improved screw-plug and stop-valve have been fitted to the inner 
 string of casing, by which means the flow of water is stopped or otherwise controlled 
 at pleasure. Generally stated, the bore was sunk in sandstone and blue clay shales of 
 the Cretaceous Formation, Up to the 30th June [1889] the expenditure on this bore 
 was £1,514 11s. 2d., including £330 12s. 11d. for transport of boring plant and casing, 
 and £176 18s. for casing.” 
 
 ANALYSIS OF WATER BY R. Mar, GovVERNMENT ANALYST. 
 
 Total fixed salts... Se or fh “tr mre see ... 40°60 
 Organic matter... Rs er a a ee ne eee O70 
 Chlorine... sed ae one ete me na ate soy bests} 
 Sulphuric acid fhe 5 bn ae ea aor bse ae  oLBce. 
 Ammonia... 5 the ae fa uae teh =i ... trace, 
 Albuminoid ammonia Fo Rte «» ‘race. 
 
 Hardness, 2° 25’. The water is fit for domestic and other uses. 
 
 * TAMBO STATION, No. 2 BORE (Private). 
 Water flowing at the rate of 15,000 gallons per day; depth not stated; boring 
 continued.t 
 LANSDOWNE BORE (Private).—Lat 25° 8’, Long. 146° 13’. 
 
 Depth, 2,485 feet ; water rises to within seventeen feet of surface.t 
 
 GRIFFITH’S BORE, ten miles east of Muttaburra.—Lat 22° 37’, Long. 144° 32’. 
 
 Depth, two hundred and ninety-three feet. The prevailing strata were fine- 
 grained grey sandstones, with some grey shales similar to those in the Aramac Well. 
 Specimens of Jnoceramus, &c., were obtained at two hundred and seventy-four feet.§ 
 
 ARAMAC,—Lat. 23°, Long. 145° 15’. 
 
 The “ Town Well,” Aramac, was sunk to the depth of three hundred feet, in or 
 before 1885. A section of the strata met with has already been given (p. 405). 
 The shaft was five feet by three feet. Salt water was struck.at forty-seven feet, and 
 made five feet in twenty-four hours for some time, but in October, 1885, had diminished 
 to three feet. A trifling amount of fresh water was met with at ninety-eight feet. 
 
 Artesian water has been met with on Aramac Run in two private bores. No. 1, 
 six hundred and fifty feet deep, yields 2,000,000, and No. 2, 1,011 feet deep, yields 
 1,750,000 gallons of overflowing water daily. The temperature of the water is 81° in the 
 ease of No. 1 Bore, and 99° in the case of No. 2. The pressure per square inch is— 
 No. 1, 25 lb.; No. 2, 89 lb.+ 
 
 The following items of information regarding wells in the Aramac District were 
 supplied to me in October, 1885, by Mr. William Forsyth :— 
 
 (1.) Aramae Run, eight miles above Aramac.—Bore, one hundred feet deep ; no 
 water; strata as in Aramac Well. 
 
 * Hydraulic Engineer’s Report, 30th June, 1889, 
 
 + Ibid., 30th June, 1891. 
 
 + Brisbane Courier, 27th October, 1892. 
 
 § Information supplied by Mr. William Forsyth, manager of Aramac Station, 
 
426 
 
 (2.) Ten miles up creek from Aramac.—Bore, one hundred and eighty-seven feet ; 
 no water; strata as in Aramac Well. 
 
 (3.) On right bank of Aramac Oreek, ten miles above Aramac.—Bore, two 
 hundred and twenty-seven feet; no water; strata as in Aramac Well. ‘The bore is 
 near some springs which are said to break out only in dry seasons. 
 
 LEICHHARDT DOWNS, near Aramac, 
 
 “ A second supply of artesian water has been struck on that Selection, the yield 
 being 280,000 gallons per day. The depth of the bore is 2,488 feet. This is the second 
 bore on Leichhardt Downs, the No. 1 having tapped water which flows at the rate of 
 1,000,000 gallons per day.’’* 
 
 CALEDONIA STATION, Aramac. 
 
 Depth, five hundred and seventy-seven feet; water overflowing at the rate of 
 100,000 gallons per day.t 
 
 NORTHAMPTON DOWNS.—Lat. 24° 32’, Long. 145° 50’. 
 
 The following information regarding wells on Northampton Downs was supplied 
 in 1885, by the late Mr. F. R. Murphy, M.L.A., the Proprietor of the Run :— 
 
 (1.) Coomdarmah Block, south bank of Barcoo, three miles back from river. 
 Depth, one hundred and twenty-five feet. Small supply of fresh water. 
 
 (2.) Glenusk Block, north bank of Barcoo, four miles from river. Depth, 
 one hundred and fifty feet. Small supply of fresh water. 
 
 (3.) Northampton Block, north side of Barcoo, ten miles from river. Depth, 
 two hundred feet. Small supply of water, as salt as brine. 
 
 (4.) Same Block, north side of Barcoo, five miles back from river. Depth, one 
 hundred and eighty feet. Fair supply of water, but brackish and unfit for stock. 
 Northampton Downs Private Bore. Depth, 1,334 feet; overflow, 25,000 gallons 
 per day.t 
 
 DARBY POINT BORE (Government).—Lat, 25° 30’, Long. 146° 30’. 
 
 This bore is situated about midway between Augathella and Tambo. It was 
 abandoned after “it had reached a depth of six hundred and sixty-two feet in sand- 
 stone and shales of the Cretaceous Formation.’’§ 
 
 STEWART’S BORE (Government).—Lat. 24° 20’, Long. 146° 20’. 
 
 This bore is in the Desert Sandstone Formation, under which heading see 
 Remarks (Chapter xxxiii.) 
 
 WELLSHOT BORE (Government).—Lat. 23° 33’, Long. 144° 55’. 
 
 “This bore is situated about six and a-half chains southerly from the 370 
 miles 33 chains peg from Rockhampton, on the proposed extension of the Central Rail- 
 way from Barcaldine to Longreach, and its altitude is about eight hundred and fifty- 
 seven feet above sea-level.” The bore was abandoned at 1,160 feet, owing to the loss 
 of tools. “The strata bored were clay, shales, and sandstones of the Cretaceous 
 Formation.’’§ 
 
 * Brisbane Courier, 12th December, 1891. 
 
 + Brisbane Observer, 9th November, 1891. 
 
 { Hydraulic Engineer’s Report, 30th June, 1891. 
 § Lbid., 30th June, 1889, 
 
427 
 
 TARA. No. 3 BORE, Wellshot Run, near Barcaldine (Private). 
 
 Water struck at 1,930 feet; supply, 20,000 gallons perday. At 2,033 feet the 
 volume had increased to 75,000 gallons, and at 2,050 feet to about 150,000 gallons. At 
 2,100 feet the supply was between 150,000 and 200,000 gallons. Still sinking. The 
 temperature at 1,930 feet was 110°, and it gradually increased to 135° at 2,100 feet.* 
 
 ADAVALE.—Lat. 25° 55’, Long. 144° 36’. 
 In 1885 I visited a well at Adavale, which had been sunk to a depth of one 
 hundred feet through white shales. Very salt water was standing fifty feet deep. The 
 site of the well is about 1,000 feet above sea-level. 
 
 GUMBARDO SAWMILL WELL, near Adavale.—Lat. 26° 10’, Long. 144° 45’. 
 
 In passing this well, in 1891, I was informed by Mr. F. Learmouth, Manager of 
 the Station, that the total depth was seventy-five feet. The spill-bank showed that 
 fine hard shales were occasionally parted by beds of fine-grained ferruginous sandstone, 
 and that there isa very coarse siliceous grit near the bottom. A well at the Station 
 shows similar material. After my visit to the Moondilla Gold Field (see Chapter 
 xxxy.), [am inclined to suspect that the strata cut in this and the preceding bore 
 may prove to be Tertiary, and not Cretaceous. 
 
 CHARLEVILLE BORE (Government).—Lat. 26° 26’, Long. 146° 15’. 
 
 “This bore is situated within a few yards of the Railway Terminus, and its 
 altitude is nine hundred and seventy-five feet above sea-level.”” ‘The strata pierced 
 may be briefly stated as follows, viz.:—Sand, clays, and gravels of the Upper Cretaceous 
 [Desert Sandstone?] Formation to two hundred and seventy feet; thence clays, 
 sandstones, and light-coloured shales of the Lower Cretaceous Formation, interstratified 
 with thin. beds of gravel to eight hundred and seventy-five feet ; thence well-defined 
 blue shales of the latter formation to the bottom in sandstone, where the large supply 
 of water was found. From one hundred and seventy-five to one hundred and ninety-five 
 feet from the surface excellent fresh water was struck in gravel, but it did not flow. 
 At three hundred and ten feet a further supply was tapped, and the bore was finished 
 at 1,370 feet 10 inches. It is lined with two strings of A. and J. Stewart’s swollen- 
 jointed wrought-iron casing. The outer string consists of two hundred and fifty- 
 eight feet of ten-inch tubes, 14+ inches thick; the inner of 1,219} feet, eight inches in 
 diameter, 3%; inches thick. Before inserting and fixing the plug and valve 
 for controlling the flow, the water was spouting with a velocity of fully eleven feet per 
 second, and to a height of about three feet above the top of the eight-inch casing. On 
 closing the valve the pressure was found to be 95 lb. per square inch, which has since 
 increased to 100 lb. The volume is now fully 3,000,000 gallons per twenty-four hours. 
 The water is clear, colourless, soft, and potable. Its temperature is about 106° 
 Fahr., and when coo! it is, as far as I can judge, wholesome and palatable. For a little 
 time after the plug was inserted the valve was occasionally choked by large pieces of 
 shale, which the water brought from the bottom, and the valve had to be frequently 
 taken off to clear it. This inconvenience was remedied as follows :—One hundred 
 and ninety-three feet of six-inch casing were screwed together, the lower sixty-three 
 feet of which were well perforated and then allowed to drop to the bottom, the top of 
 the six-inch casing overlapping the eight-inch by forty-two and a-half feet. This 
 mode of dealing with the difficulty had the desired effect ; no trouble has accrued since. 
 By this means the flow and pressure have been maintained intact, and, so far as I 
 
 
 
 
 
 * Rockhampton Bulletin, December, 1891, 
 
428 
 
 am aware, this well may be pronounced the best in Australia, as far as regards volume* 
 although the pressureis not so great as at Cunnamulla, where it is fully 185 lb. per 
 square inch.t When the valve is fully opened, and a ‘director’ with an orifice of 
 one and a-half inches is fitted thereon, the water shoots to a height over one hundred 
 feet from the surface. The cost was £2,388 14s. 5d., including supervision of the work, 
 and £86 8s. 5d. for caretaking to 30th June last”’ [1889]. 
 
 In the 1890 Report, Mr. Henderson gives the following analysis of the water by 
 Mr. R. Mar:—“ Total fixed salts 70°70, nies 12°95, hardness 3°; and a note is 
 appended that the water is “ unfit for irrigation—may be sed for other purposes.” 
 
 In an article by Mr. Ludwig Bruck on ‘‘ The Mineral Springs of Australia’’§ is 
 the following note on an analysis (furnished by the Department of Mines) of water 
 from “Charleville district,” which I presume to refer to the Charleville Artesian 
 Well :— 
 
 “ This water is of a strong saline character, and contains 604°78 grains of mineral 
 matters per gallon, viz.:—Chloride of sodium, 347°42 gr.; chloride of lime, 100°59 gr.; 
 chloride of magnesium, 63°89 gr.; sulphate of ahd 79°27 er.; and 13°61 gr. carbonate of 
 lime. This spring contains so Sore chloride of lime as to make it unfit for drinking 
 purposes; however, used as baths it would no doubt be found useful in scrofula, enlarge- 
 ment of the liver, and derangement of the spleen; ata tepid temperature (say from 85° 
 to 94° F.) it should be useful in cutaneous diseases, and taken as hot baths (from 98° to 
 112° F.) in rheumatic and similar affections. I cannot say whether this water is identical 
 with the water struck at the same place in a bore 1,350 feet deep, the temperature of 
 which is over 112° F.”’ 
 
 MURWEH BORE (Private).—Lat. 26°58’, Long. 146° 20’. 
 Depth, 1,230 feet; overflow, 140,000 gallons per day; temperature, 98°. 
 
 MUCKADILLA BORE (Government).—Lat. 26° 40’, Long. 148° 20’. 
 This bore is near Muckadilla Station, on the Western Railway, six miles east of 
 Dalby. Itis3,262 feet deep, being the deepest in the Colony, or indeed in the Australian 
 Colonies. The following section has been supplied to me by Mr. Henderson :— 
 
 Feet. Depth. 
 Yellow clay ... see ae See ee TOU 
 Black shale... ae ie a ae as net de 
 Sandstone a oe Ore sa i see ete Pe ae 
 Black shale... at sae as “ri w. «6234 ie 678 
 Grey pipeclay ... ee ae ue oF rie eB bis 794 
 Grey sandstone - neem ciaces ie aeleo 43 989 
 Sand drift, white and lignite ; tapped water... 21 7 1,010 
 Shale, brown and grey ie Sy i. ae ue aie 1,071 
 Sandstone conglomerate, grey fs Sa ee AG es 1,097 
 Shale, brown and grey 6 Ge | Ok = 1,151 
 Sand drift, white and brown; Weter inoreased ee aey! see 1,278 
 Shale, brown ... She ak Pee wae eee an 1,293 
 Sand drift, grey a we Wee ee Mee ai 1,325 
 Shale, grey, siliceous... at ae eh: Bao WR} ee 1,448 
 Sandstone, brownish grey ... ie et ~~ (85 ae 1,533 
 Sand drift, white and grey ... a. ay ww 148 sa 1,681 
 Shale, blackish ne es a oo ee DO) nas 1,831 
 
 
 
 * See Noorama and Burranbilla Bores. 
 
 + An Artesian Well in Dakota has a reported pressure of 200 1b. per square inch—the greatest I 
 have any knowledge of. 
 
 + Annual Reports of the Hydraulic Engineer, 30th June, 1889 and 1890. 
 
 § Australasian Medical Gazette for January, 1891. 
 
 —_—T 
 
429 
 
 Feet. Depth. 
 Sandstone, grey Ae adc. 20 see 1,860 
 Shale, slate-coloured to Trowuiehe ree ro nici ae #5 1,958 
 Shale, black, with streaks of coal . re ee at7 aA 2,235 
 Sandstone and shale, soft ... aay : isn 200 aes 2,509 
 Sandstone, white; water flowing 10, 000 gallons 
 per day ... oe 618 ee 3,118 
 Sandstone, micaceous; Ayeriow of ps 12, 960 
 gallons per day at 3, IGG teetoau cc. | rte 52 3 3,170 
 Sandstone, white and soft; water overflowing a 
 rate of 23,000 igo per tae temperature, 
 i 2 oa tac ad tet tee Bee sta OZ sed 3,262 
 ANALYSIS OF THE WaTER By R. Mar, GovernmMEeNT ANALYST. 
 Total fixed salts ... a vee oe ane te if wv» 34°80 
 Carbonate of calcium .., Ae xe in ae fre seo ALGO 
 Carbonate of magnesium ... : A f as 1.» trace. 
 Chlorides and carbonates of seat and pobissintn Ae et singe eM righ 
 Oxide of iron 4p Se we pare | SS 
 
 The water is fit for domtesti ae Stier purposes. 
 
 MITCHELL BORE (Government).—Lat. 26° 35’, Long. 147° 50’. 
 
 A bore was sunk here for the Railway Department in 1885, two hundred yards 
 west of the station. I was informed by Mr. John Falconer, who was in charge of 
 the bore, that the section showed one hundred and eighty-eight feet of blue shales 
 beneath twenty feet of drift. Water was met with at two hundred and eight feet in 
 a “sandy drift’ beneath the shales, and rose to nine feet from the surface. On the 
 3rd October, 1885, I saw it standing twenty-eight feet from the surface. The water 
 would supply, by pumping, eight hundred to 1,000 gallons per day. The site of the 
 bore is 1,101 feet above sea- level. ri 
 
 BURENDA BORE (Private).—Lat. 25° 57’, Long. 146° 50’. 
 Depth, 1,900 feet; water rises to within thirty feet of surface. 
 
 BOLLON OR SIXTY-FIVE MILE BORE (Government),—Lat. 28° 3’, Long. 147° 55’. 
 
 This bore is situated about sixty-five miles from St. George, on the road to 
 Cunnamulla. In July, 1891, the depth of 1,840 feet had been attained, and water was 
 overftowing at the rate of 30,000 gallons per day. Strata:—Alluvium, clay, sand, 
 pipeclay, limestone, dark and grey-coloured clay, shales, and sandstones of various 
 texture, interstratified in irregular order, the last stratum being coarse grey sandstone.* 
 
 I am informed (21st September, 1891) that the bore has been stopped at 2,362 
 feet, the overflow being about 180,000 gallons per day, at a temperature of 125°. 
 
 CUNNAMULLA BORE (Government).—Lat. 28° 5’, Long. 145° 40’. 
 
 “In February [1889] a supply of artesian water was struck at nine hundred and 
 seventy-five feet, but boring operations were continued in the hope of striking a larger 
 supply. As boring was continued the flow increased, until, on the 21st of February, a 
 supply of 22,500 gallons per hour [equal to 540,000 gallons per day] of excellent fresh 
 water was tapped at a depth of 1,402 feet. Its temperature is 106° F., and its pressure 
 is fully 185 lb. per square inch at the surface. On completion of boring operations the six- 
 inch casing was fitted with a recessed screw-plug and stop-valve, by means of which the 
 flow of water is controlled, and at pleasure supplied to consumers. The cost of this bore, 
 
 
 
 * Hydraulic Engineer’s Report, 30th June, 1891. 
 
430 
 
 including a sum of £488 19s. 2d. for the carriage of the plant and casing from Charleville, 
 and £403 for casing, was £1,927 17s. 5d. Generally stated, the strata pierced were 
 clays, shales, and light sandstones of the Cretaceous formation.”* 
 
 In his next Annual Report Mr. Henderson observed that “This work is in 
 excellent order, but the high pressure of the water, which I believe has increased from 185 
 to 190 lb. per square inch, is very trying on the valve. A new one of superior design 
 and stronger make will shortly be sent out to replace the old one, which has partly given 
 way. 
 
 ANALYSES BY R. Mar, GOVERNMENT ANALYST. 
 
 First. Second. 
 Total fixed salts ... See ae ne a. 22 10 a 25°75 
 Organic matter... ive so hn s.. brace oe trace 
 Chlorine oe an Mg wee ... trace ane 0°70 
 Ammonia oe a ex nb i OOLS os ‘0016 
 Albuminoid ammonia aoe was eee COOLE ee ‘0012 
 
 Hardness, 3°. The water is suitable for general domestic use. T 
 
 CAWARRA, No. 1 BORE, twenty-five miles east of Hungerford.—Lat. 29°, Long. 144° 50’. 
 
 In this bore, at the depth of 1,810 feet, a supply of water was met with which 
 overflows at the rate of 10,080 gallons per day. I have been shown a specimen of 
 gneiss, which is said to have been the rock pierced from 1,600 to 1,810 feet. 
 
 BURRANBILLA BORE (Private).—Lat. 28° 20’, Long. 145° 45’, 
 Depth, 1,811 feet ; overflow per diem, 4,000,000 gallons ; temperature, 124°. 
 If the measurements are correct, this bore has the largest amount of overflowing 
 water of any in Queensland, and the water has the highest temperature. 
 
 TINNENBURRA BORES, Warrego River (Private).—Lat. 29°, Long. 145° 35’ 
 
 
 
 
 
 
 
 
 
 — Depth. Overflow per day. Casing. preside 
 Gallons. Inches. Inches. 
 Novi ee, | ae eT 350 500,000 8 4 
 Sy eae Abe Sen Aor ae 993 1,500,000 6 26 
 Hone rE oe Aer Ane 1,293 250,000 6 0:2 or 3 
 on At was oe ee ee 855 800,000 8 —5 
 5 ON ee <i ae ie 1,300 
 
 NOORAMA BORES (Private).—Lat. 28° 20’, Long. 146°. 
 
 No. 1 Bore. 1,502 feet deep; overflow, 1,500,000 gallons daily ; temperature, 
 112°; pressure, 200 lb. 
 
 No. 2 Bore.’ 1,650 feet deep ; overflow, 1,500,000 gallons daily. 
 
 No. 3 Bore. 1,632 feet deep ; overflow, 3,456,000 gallons daily ; temperature, 
 112°; pressure, 200 lb.+ 
 
 Writing on 11th September, 1890, Mr. Henderson, in his “ Annual Report for the 
 Year ending 380th June,” adds to the paragraph on the Charleville Bore a footnote in the 
 following terms, probably referring to the Noorama Bore :—“ Since this was written it 
 has been reported through a business house in this city that a bore in the Cunnamulla 
 
 
 
 * Hydraulic Engineer’s Report, 30th June, 1889. 
 + Ibid., 30th June, 1891. 
 
 + Information furnished to Mr. McLennon, of the Hydraulic Engineer’s Department by Mr. Joseph 
 Pater. 
 
 § “A good supply of fresh water. . . . . remarkably hot.”—Brisbane Courier, 21st March, 1892, 
 
431 
 
 district has very lately tapped a supply of nearly three and a-half millions of gallons per 
 diem. The Ponce de Leon well at St. Augustine, Fla., U.S.A., has an estimated daily 
 discharge of 10,000,000 gallons—doubtless U.S. gallons. The well is 1,400 feet deep by 
 twelve inches diameter. The temperature of the water is 82° Fahr. This is the largest 
 discharge of any well I know of.” 
 
 WEELAMURRA BORE (Private),—Lat. 28° 15’, Long. 146° 15’, 
 Depth, 1,589 feet; water overflowing at the rate of 150,000 gallons per day; 
 temperature, 1133°; pressure, 150 lb. to the square inch.* 
 A newspaper report states that at five hundred and seventy feet, in black shale 
 clay, the (No. 3?) bore struck alkaline water, which rose five hundred feet in the tubes. 
 
 BURRENDILLA BORE, near Cunnamulla (Private). 
 Water overflowing at the rate of 2,500,000 gallons per day; depth not stated. 
 
 DILLALAH BORE, about fifteen miles from the Warrego. 
 Depth, 1,300 feet; water overflowing at the rate of 250,000 gallons per day. 
 “ Almost fresh and quite soft.’’§ 
 
 THARGOMINDAH BORE. ~ 
 “Fresh water was struck at a depth of 1,100 feet, and the water has risen within 
 one foot of the surface. Boring is being continued.”’|| 
 
 BARRINGUN, WARREGO RIVER (just across the New South Wales Border), 
 Water overflowing at the rate of about 25,000 gallons daily; still boring.4] 
 
 MALVERN, HILLS BORE. 
 Depth, 2,800 feet ; water struck at 1,300 feet, but did notrise to the surface.** 
 
 KUNGIE LAKE BORE, forty-five miles south-west of Cunnamulla (Private).—Lat. 28° 40’, Long. 145° 18’. 
 Depth, 1,255 feet; overflow, 500,000 gallons per day; temperature, 110°. 
 
 THURLAGOONA BOREKHS (Private).—Lat. 28° 50’, Long. 145° 30’. 
 No.1. Depth, 1,270 feet; overflow, 177,000 gallons daily ; temperature, 112°. 
 No. 2. Depth, 1,440 feet ; yield per diem, 30,000 gallons ++; temperature, 102°. 
 No. 3. Depth, 1,616 feet; overflow per diem, 200,000 gallons ; temperature, 108°. 
 No. 4. Depth, seven hundred and eighteen feet; yield per diem, 86,000 gallons ft ; 
 
 temperature, 102°. 
 No. 5. Depth, eight hundred and thirty-one feet; overflow per diem, 8,000 
 
 gallons.tf 
 No.6. Depth, 1,529 feet; overflow per diem, 1,500,000 gallons; tempera- 
 
 ture, 108°. 
 CHARLOTTE PLAINS, near Cunnamulla,—Lat. 28° 20’, Long. 146° 10’. 
 
 This Run is situated on Widgeegoara Creek. Artesian water has been met with 
 at 1,662 feet. The yield is 570,000 gallons per day.§§ 
 
 * Hydraulic Engineer’s Report, 30th June, 1891. 
 t+ Townsville Bulletin, 21st December, 1888. 
 t Brisbane Courier, 25th June, 1891. 
 § Ibid., 2nd March, 1892. 
 || Zbid., 5th March, 1892. 
 { Ibid., 24th March, 1892. 
 ** Rockhampton Bulletin, December, 1891. 
 +t Overflowing slightly ; supply pumped. 
 +t Salt water ; overflowing when first tapped, but has since receded. 
 §§ Sydney Lvening News, 10th April, 1891, 
 
 
 
432 
 
 COONGALLA, near Cunnamulla.—Lat, 27 45’, Long. 145 50’. 
 No. 1 Bore at 1,600 feet tapped water overflowing at the rate of 1,000,000 
 gallons per day.* 
 No. 2 Bore “struck a good supply of beautiful water, estimated to yield 
 2,000,000 gallons daily, at a depth of 1,800 feet.”’+ 
 
 CLAVERTON BORKES, near Cunnamulla. 
 No.1 Bore. Estimated yield, 3,000,000 gallons per day; depth not stated. f° 
 No. 2 Bore. Depth, 1,250 foen, water overflowing at the rate of 20, 000 
 gallons per day.§ ‘Struck a big supply of fresh water on the 15th instant, the flow 
 being estimated. at 1,550,880 gallons daily, the pressure being 166 lb. to the square 
 inch. The depth is 1,777 feet, and the supply is excellent.” 
 
 BUNDILLA BORE, Bundilla Creek, Bingara Station, near Eulo (Private). 
 Water at 1,675 feet. “A good supply.” Amount not stated. ‘“ The water is 
 very hot, clear as crystal, and quite fresh.”’|| 
 
 WHITULA, near Windorah.—Lat. 25 20’, Long. 142° 10’. 
 This bore has been carried to over 2,000 feet without success.4 
 
 SANDRINGHAM BORE (Private).—Lat, 24° 25’, Long. 188° 55’. 
 
 A. newspaper report states that at Sandringham Station, on the Mulligan River, 
 thirty-five miles west of Bedoworie Township, a supply of water overflowing at the rate 
 of 40,000 gallons per day has been struck at the depth of one hundred and forty-three 
 feet. Bedoworie is on Eyre’s Creek, about fifteen miles north of its junction with 
 King’s Creek. 
 
 A second bore on Sandringham, between the Mulligan River and Sylvester 
 Creek (Lat. 23° 30’, Long. 138° 55’), has, I am informed by Mr. G. Neville Griffiths, been 
 sunk between two springs to the depth of one hundred and sixty feet, and supplies 
 180,000 gallons of overflowing water daily. 
 
 BREADALBANE BORE,.—Lat. 23° 50’, Long. 139° 15’. 
 A bore is being sunk here near the “ Three Sisters,” twenty-seven miles up 
 Coemerino Creek, Georgina River. The following section has been supplied by Mr. G. 
 Neville Griffiths, the owner of the station :— 
 
 Feet. 
 
 Clay, sand, and gravel drift (with traces of soda and SEs 30 
 Strong blue clay shale (brackish ota cr ‘< Soro 
 Soft blue shale Ke ioe ean wete LG 
 . » (slightly cufforentn in recta} us ee .. 934 
 Hard sandstone band a ox aaa sa ra i 1 
 Blue shale... : as: $4 a see ae ue aoe 
 Hard sandstone band me os we eee oe ae 1 
 Blue shale... 168 
 
 (Strong flow of slightly Sees Teens which rose sto tasty foot 
 from surface) 
 
 
 
 * Brisbane Courier, 1st October, 1891. 
 + Ibid., 10th March, 1892. 
 
 t Ibid., 12th November, 1891. 
 
 § Ibid., 18th February, 1892. 
 
 || Lbid., 15th December, 1891. 
 
 4 Ibid., 27th November, 1891. 
 
433 
 
 Feet, 
 Hard blue shale __.. ne ie as ae hie 
 Hard blue shale with black pebbles ay ase ae 2 
 Fine dark gritty sandstone.. a re aa re 3 
 (Brackish water cased off to ane bed, and erect water rises to six 
 feet from surface) 
 404, 
 
 (Bore in progress). 
 
 There are no springs nearer than the Sylvester Springs, which are referred to 
 under the head of Sandringham. 
 
 SOUTH AUSTRALIA. 
 
 Referring to the Rolling Downs Formation, as developed in South Australia, Mr. 
 H. Y. L. Brown, Government Geologist for that Colony, says *:— 
 
 ‘“‘ Below and surrounding the table-hills and stony downs are the soft silt plains, 
 which, together with the former, cover the gypseous clays, marls, calcareous shales, 
 limestone, sand, and gravel drifts of Cretaceous age. The greatest thickness of these 
 beds, which has been ea by boring at Tarkininna, is about 1,200 feet. The mound 
 springs, which are the natural indications of artesian water beneath these plains, are 
 found in many places near the outcrops of bed rock, between the junction of which and 
 the Cretaceous rocks the water has, doubtless, found an easier egress. On the surface 
 the water often forms accumulations of travertine limestone, rising to heights of forty 
 or fifty feet, and showing in the distance across the level plains, where there isa group of 
 springs, like a low range of hills; the deposition of this limestone has, in many 
 instances, formed raised cups or basins, over the edges of which the water flows. The 
 water of these springs contains soda, and is generally good drinking water; in some 
 cases, however, in the same group of springs, there is a great difference in the quality 
 of the water, which in one spring may be drinkable, and in another, a few feet away, 
 salt. Asa rule these spring waters are warm, and must have a considerable tempera- 
 ture beneath the surface. Bores have been sunk by the Government in this formation 
 at Tarkininna, where artesian water was tapped at 1,200 feet, and at Hergott, Coward 
 Springs, Strangway Springs, &c., where a large supply of water was obtained at an 
 average depth of some three hundred feet. The supply from some of these bores is 
 over 1,000,000 gallons per day.” 
 
 J. 
 
 
 
 *The Mesozoic Plains of South Australia, Proc. Austr, Assoc. Adv, Sci., i., 1888, p. 243, 
 2D 
 
CHAPTER XXXIT. 
 
 THE ORGANIC REMAINS OF THE ROLLING DOWNS FORMATION 
 
 (LOWER CRETACEOUS). 
 
 Wir DEscrIPrions OF THE SPECIES. 
 
 “To draw a definite line between the Ipswich and the ‘Rolling Downs’ Bed is 
 quite impracticable. The appearance of Belemnites and Ammonites generally marks 
 the transition.’’* 
 
 The physical aspect of the country produced by the former has been described 
 by my Colleague, who states that the general absence of sections renders it impossible 
 to subdivide this division, or to trace out definite horizons. He remarks—‘‘ We have 
 a continuous series of beds of enormous thickness, in which, however, from the scarcity 
 of sections, 1t would be impossible to map out horizons ;”’ and that “the fossils from 
 the Rolling Downs must be treated as a whole.’’+ In the latter part of this paragraph 
 I cordially agree, and have for some time past advocated classing the Rolling Downs 
 Beds under the general term. Cretaceous, admitting, however, at the same time that 
 they contain an admixture of Oolitic as well as Cretaceous life. Even the late Charles 
 Moore did not venture to introduce a geological sequence for the Queensland series, as 
 he did for the Mesozoie Beds of Western Australia, but contented himself by remarking, 
 “These and other circumstances indicate a higher horizon for the Queensland fossils.”’ 
 He appeared to think that the Oxford Clay put in a strong claim, but that “they all 
 belong to the Upper Oolite may with safety be inferred.” f 
 
 I cannot do better than again quote my Colleague, who adds—‘ The fossils of 
 the Rolling Downs Formation have given rise to much controversy among geologists 
 and paleontologists, who have pronounced various localities, from limited collections, to 
 be of ages ranging from Rhetic up to Lower Chalk. It is remarkable that almost 
 every paleontologist who has worked on Queensland materials has come to the 
 conclusion that fossils from different localities must have been mixed up, and this 
 explanation has appeared to be specially necessary in the ease of fossils from the 
 Rolling Downs. On the other hand, my own explorations have satisfied me that 
 Queensland fossils are not more liable to this kind of accident than fossils from other 
 countries, and that the mixing up which has so annoyed paleontologists has been 
 perpetrated by Nature herself.” 
 
 
 
 *R. L. Jack, Handbook Queensland Geology, 1886, p. 65. 
 + Ibid., p. 67. 
 +t Quart, Journ, Geol. Soc., 1870, xxvi., pp. 235 and 239, 
 
435 
 Kingdom—ANIMALIA. 
 Sub-Kingdom—PROTOZOA. 
 Class—RHIZOPODA. 
 Order—FORAMINIFERA. 
 Family—LAGENIDA. 
 
 Genus—ORISTELLARIA (Lamarck), D’ Orbigny, 1826. 
 (Ann. Sci. Nat., vii., p. 290.) 
 
 CRISTFLLARIA ACUTAURICULARIS, Ficht. and Moll, var. tonatcostata, ALoore. 
 
 Cristellaria acutawricularis, var. longicostata, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 242. 
 Fe oA var. longicostata, Eth. fil., Cat. Austr. Foss., 1878, p. 102 (for synonymy). 
 
 Sp. Char. Shell oblong, moderately bi-convex, later chambers passing beyond 
 helicoid portion ; surface with ribs which are longitudinally costated. (Jfoore.) 
 
 Obs. The typical European forms of C. acutauricularis which are found also with 
 this shell possess smooth surfaces, and are without the longitudinal costa —the difference 
 being so marked as to justify its separation. (Joore). 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 CRISTELLARIA CULTRATA, Montfort, var. RADIATA, Moore. 
 
 Cristellaria cultrata, var. radiata, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 242. 
 3 5 var. radiata, Eth. fil., Cat. Austr. Foss., 1878, p. 103 (for synonymy). 
 
 Obs. This shell possesses the central disk of C. cultrata, from which the ribs on 
 the surface proceed ; and although the keel is less produced, there appears no doubt 
 that it must be referred to this species. From the more radiating character of the 
 coste the varietal name of 0. radiata was proposed. (dLoore.) 
 
 Loe. Wollumbilla (The late Rev.. W. B. Clarke). 
 
 Genus —DENTALINA, D’ Orbigny, 1826. 
 (Ann. Sci. Nat., vii., p. 254.) 
 
 DenTALINA comMuUNIS, D’ Orbigny. 
 
 * 
 Dentalina communis, D’Orb., Mém. Soc. Géol. France, 1840, iv., p. 18, t. 1, f. 4. 
 bps A Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 239. 
 
 Obs. This species was recorded by the late Mr. Charles Moore without either 
 description or observations. 
 Loc. Wollumbiila (Lhe late Rev. W. B. Clarke). 
 
 Genus—VAGINULINA, D Orbigny, 1826. 
 (Ann. Sci. Nat., vii., p. 257.) 
 
 VAGINULINA STRIATA, D’ Orb, 
 
 Vaginulina striata, D’Orb., Ann. Sci. Nat., 1826, vii., p. 257, 
 s . Moore, Quart. Journ, Geol. Soc., 1870, xxvi., Pt. 2, p. 239. 
 "5 oe Eth. fil., Cat. Austr. Foss., 1878, p. 104 (for synonymy). 
 
 Loc, Wollumbilla (Lhe late Rev. W. B. Clarke), 
 
436 
 
 Genus—POLYMORPHINA, D Orbigny, 1826. 
 (Ann. Sci. Nat., vii., p. 265.) 
 
 PoLtywMoRPHINA GIBBA, D’Orb., sp. 
 
 Globulina gibba, D’Orb., Ann. Sci. Nat., 1826, vii., p. 266. 
 Polymorphina gibba, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 239. 
 Ap 55 Eth. fil., Cat. Austr. Foss., 1878, p. 104 (for synonymy). 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 PoLYMORPHINA LACTEA, Walker and Jacob, sp. 
 
 Polymorphina lactea, Parker and Jones, Ann: and Mag. Nat. Hist., 1859, iv., pp. 336 and 341. 
 35 : Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 239. 
 < i Etheridge fil., Cat. Austr. Foss., 1878, p. 104 (for synonymy). 
 
 Loc. Wollumbilla (Zhe late Rev. W. B. Clarke). 
 
 “Family—ROTALIDZ. 
 
 Genus—PLANORBULINA, D Orbigny, 1826. 
 (Ann. Sci. Nat., vii., p. 280.) 
 
 PLANORBULINA LOBATULA, D’Orb., sp. 
 
 Truncatulina lobatula, D’Orb., Foram. Foss. Tert. Vien., 1846, p. 168, #..9, £. 18-23; 
 Planorbulina lobatula, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 289. 
 3 7 Eth. fil., Cat. Austr. Foss., 1878, p. 103 (for synonymy). 
 
 Obs. No remarks were made on this species by Mr. Moore. 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 PLANORBULINA UNGERIANA, D’ Orbigny, sp. 
 , gny 
 
 Rotalia ungeriana, D’Orb, Foram. Foss. Tert. Vien., 1846, p. 159, t. 8, f. 16-18. 
 Planorbulina ungeriana, Moore, Quart. Journ. Geol. Soc., 1870, xxvii., Pt. 2, p. 239. 
 e oe Eth. fil., Cat. Austr. Foss.,.1878, p. 104 (for synonymy). 
 
 Obs. Like the two last, this is only a list species. 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Class—SPONGIDA.* 
 
 Order—SILICISPONGIA. 
 Sub-Order—HEXACTINELLIDA. 
 Group—LYSSAKINA. 
 
 Genus—PURISIP HONTA, Bowerbank, 1869.+ 
 
 Purisiphonia, Bowerbank, Proc. Zool. Soc., 1869, p. 342. 
 
 Bowerbank, in Moore, Quart. ee Geol. Soc., 1870, xxvi_p. 240. 
 
 Carter, Ann. and Mag. Nat. Hist., 1878, i., p. 376. 
 
 Zittel, Handb. Pal., 1876, i., p. 179. 
 “Gen. Char. The form of the entire sponge is unknown. Judging from the 
 portions preserved, it appears to have consisted of a hollow stem giving off tubular 
 branches. The walls are thick and robust, and the outer surface slightly uneven. 
 
 39 
 
 ” 
 
 
 
 *The present article on Purisiphonia has been kindly contributed by Dr. George Jennings Hinde, 
 from specimens in the Natural History, Museum, London. It is given verbatim in his own words. 
 + Emend, Hinde, 1892, . 
 
437 
 
 . 
 
 “The wall of the sponge is traversed by numerous canals, which open on both sides 
 of the wall, and extend inwards, either at right angles or obliquely to the surface of 
 the sponge. The canals bifurcate or branch within the wall; they do not penetrate 
 through it, but terminate just below the opposite surface to that on which their oscules 
 open. There is no definite arrangement in the course of the canals, which occasionally 
 appear to anastomose within the wall. The canals are evenly bounded by the ordinary 
 spicular tissue, and do not possess a special lining. The oscular apertures are either 
 circular, elliptical, or trumpet-shaped, and in some instances divided by the extension 
 over them of the spicular fascicles. 
 
 “The skeletal mesh composing the substance of the sponge-wall is close, resistant, 
 and intricate. It consists of slender fascicles or bundles of straight, elongate, linear 
 spicules, disposed parallel with each other, and united together by a common coating 
 of silica throughout the greater part of their length. These spicular fascicles have no 
 definite arrangement; they overlap each other in different directions, though for the 
 most part they are generally parallel with the sponge-wall. They are more abundant 
 on the exterior surfaces, though they also traverse the interior of the wall in various 
 directions. Between these fascicles there are rod-like spicules, either nearly parallel 
 with each other or disposed irregularly, crossing and intercrossing each other in all 
 directions. At their points of contact these spicules are definitely fused together, and 
 they are further united by the development of short transverse rods and siliceous pro- 
 cesses which connect adjoining, spicules, and thus form a strong and complex spicular 
 mesh-work with irregular interspaces. Here and there in the interspaces of the mesh 
 are solitary regular hexactinellid spicules, their rays being fused with the adjacent 
 mesh-work, and in many places also there are small groups of minute regular 
 hexactinellid spicules, intermingled closely together without any order, and their rays 
 fused at the points of contact with each other. + 
 
 “There is no apparent specialised dermallayer. On both surfaces of the sponge- 
 wall the spicular fascicles extend over the oscular vents, and the spaces between the 
 fascicles exhibit much the same spicular character as the interior of the wall. Further, 
 the canals are not lined by any distinctive spicular tissue. 
 
 “Obs. “ Mr. H. J. Carter has truly remarked of this genus that its minute spicular 
 structure is totally different from that of any other hexactinellid sponge. Its peculiar 
 characters render its relationship somewhat doubtful. At first sight, indeed, one would 
 hardly recognise it as a hexactinellid sponge, since only the fascicles of linear spicules 
 are exposed on its surface, and the intermediate scaliform or irregular spicular tissue 
 more resembles a combination of monactinellid than hexactinellid spicules. The pre- 
 sence, however, of definite six-rayed hexactinellid spicules, either singly or forming 
 small groups in the interspaces of the mesh-work, at once determines its relations to 
 this order. Its position within the order is less easy to define. The entire absence of 
 any regular arrangement of the spicular mesh, or of any regular tissue formed by the 
 fusion of the rays of regular hexactinellid spicules with the corresponding rays of 
 adjacent spicules, removes the genus from the Dictyonine Group of the Hexactinellide. 
 The definite fusion of the spicular rays with each other, thus binding them firmly 
 together, is, on the other hand, a character which would tend to exclude this genus from 
 the Lyssakine Group, in which, as a rule, the spicules are only held in position by the 
 soft animal structures of the sponge. Notwithstanding this fact, the general 
 spicular characters of Purisiphonia appear to me to indicate a closer relationship to the 
 Lyssakina than to the Dictyonina. 
 
 “Thus the fascicles of spicular rods may be compared with those of the existing 
 genus Huplectella, Owen, though they are not continuous as in the recent form, and a 
 
438 
 
 further resemblance is shown in the fact that in this recent genus also the linear and 
 other spicules are partially united in an irregular manner by transverse bulks and 
 siliceous extensions as in Purisiphonia. Likewise in the existing genera, Hertwigza, 
 O. Schmidt, and Rhabdopectella, O. Schmidt, the skeletal spicules are firmly cemented 
 together in the lower portion, whilst they are free in the upper portion of the sponge, 
 thus exhibiting, as Oscar Schmidt remarks,* transitional characters between the 
 Lyssakina and Dictyonina. These recent genera have been, however, ranked with the 
 Lyssakina Group, and, considering the nature of the spicules in Puwrisiphonia, it should, 
 in my opinion, also be placed in thesame group. In its massive wall of closely arranged 
 spicular fibres, all firmly and irregularly cemented together, and penetrated by definitely 
 bounded branching canals, this genus is very distinctly marked off from any other 
 Hexactinellid, whether fossil or recent. 
 
 PurRiIstPHONIA CLARKEI, Bowerbank, Pl. 19. 
 
 Purisiphonia Clarkei, Bowerbank, Proc. Zool. Soc., 1869, p. 342, Pl. xxv., figs. 6 and 7. 
 
 Moore, Quart. Journ. Geol. Soc., 1870, xxvi., pp. 235, 240, Pl. xvii., fig. 1. 
 
 Sollas, Quart. Journ. Geol. Soc., 1877, xxxiii., p. 802. 
 
 Carter, Ann. and Mag. Nat. Hist., 1878, i., p. 376. 
 
 + - Zittel, Handb. Pal., 1878, i., p. 179. 
 
 Eth. fil., Cat. Austr. Foss., 1878, p. 104. 
 
 Hinde, Cat. Foss. Sponges Brit. Mus., 1883, p. 124. 
 
 Vosmaer, Bronn’s Klassen und Ordnungen des Thier-Reichs, 1885, 2 er. Bd. (Porifera), 
 
 p. 266, 
 
 “ Sp. Char. The largest fragment of this species which has vet been discovered is 
 apparently the main tubular stem of an individual with the bases of two or three 
 branches. The fragment is about one hundred mm. in length and breadth, and the 
 walls are about fifteen mm. in thickness. 
 
 “The oscules are numerous, disposed without regular arrangement, from one to 
 two mm. apart, and varying from one to three mm. in diameter. The canals very 
 slightly diminish in their course in the wail until they bifurcate. 
 
 “The spicular fascicles of the skeleton are about twelve mm. in length and from 
 fifteen to twenty-five mm. in thickness, the linear spicules composing them, about nine 
 or ten in number, are in close contact and so united by silica that the compound 
 character of the bundle can in some cases only be clearly seen by the axial canals of the 
 spicules (PI. 19, fig. 6). The linear spicules, not in fascicles, are, as a rule, much stouter 
 than those forming the fascicles ; the connecting transverse processes are numerous, and 
 so bridge over the spaces between the spicules that but little moretbhan oval or circular 
 fenestre exist between them. Though, as a rule, these connecting bulks are stouter 
 than the spicules, there are no canals present in them, whereas they can be traced in 
 most of the linear spicules. The groups of minute normal hexactinellid spicules appear 
 to be very irregular in their distribution; in some instances they are massed near 
 the terminations of the canals. Their rays appear to be sub-equal, cylindrical, or 
 tapering but very slightly and with rounded ends. The rays vary from ‘1 to ‘13 mm. 
 in length, and ‘02 mm. in thickness. These spicules, as shown in the figure (Pl. 19, 
 fig. 10), are very indiscriminately mingled together, and their rays are fused wherever 
 they are in contact with others, 
 
 Obs. ‘This species was first described and figured by Dr. Bowerbank, who received 
 the specimens from Mr. Charles Moore. He constituted for them the genus Puwrisi- 
 phonia, a rather inappropriate name, since it might be thought to indicate a connection 
 with the Lithistid genus Siphonia, with which this form has nothing in common. 
 
 * Die Spongien des Meerbusen von Mexico, 2te. Abth., pp. 42 and 62. 
 
459 
 
 Subsequently Mr. C. Moore figured the largest specimen in’ the Quarterly Journal of 
 the Geological Society, and reprinted the description of Bowerbank. Eight years later 
 Mr. H. J. Carter, F.R.S., gave an emended description of the species, pointing out its 
 particular features in a much clearer manner than had been done originally. Mr. 
 Carter compared the form with the existing Dactylocalyx pumicens, Stutchbury, and 
 with Luplectella aspergillum. We also made the rare discovery of one of the flesh 
 spicules, a globular rosette, with radiating capitate rays about z,55 inch in diameter 
 (Pl. 19, fig. 11). Following Mr. Carter’s description, Prof. Zittel gave a diagnosis of 
 the genus, and placed it as a Dictyonine Hexactinellid in the family Staurodermide. 
 The character of its spicular structures generally, and the absence of hexactinellid 
 spicules in the dermal layer of both surfaces of the wall, show, however, that it cannot 
 definitely remain in this family. 
 
 “The example in the British Museum, which is the typical form studied by Dr. 
 Bowerbank, is about fifty mm. in length and the same in breadth. It has been imbedded 
 in a calcareous matrix, which has been removed by acid, and the internal structure is as 
 clearly shown asinarecent sponge. The spicular skeleton is of a whitish-grey tint by 
 reflected, and transparent by transmitted light ; between crossed nicols the silica gives 
 the tints of chaleedony. The axial canals of the spicules are now infilled with a lightish 
 brown, apparently earthy material. 
 
 “‘No other species of the genus has yet been discovered.” 
 
 Loe. Wollumbilla (Zhe late Rev. W. B. Clarke). 
 
 Sub-Kingdom—ECHINODERMATA. 
 Section—PELMATOZOA. 
 Class—CRINOIDEA. 
 
 Order—ARTICULATA. 
 Family—PENTACRINID. 
 
 Genus—PENTACRINUS, Miller, 1821.* 
 (Nat. Hist. Crinoidea, p. 45.) 
 
 PENTACRINUS AUSTRALIS, Moore, Pl. 20, f. 1-3. 
 Pentacrinus australis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 248, t. 17, f. 3, t. 18, £1, 
 
 Sp. Char. Pelvis short, compressed, rounded ; plates of the body and arms 
 finely rugose; scapule thick, supporting ten arms, composed of thirteen plates, the 
 hands bifurcating from cuneiform joints, the fingers being of considerable length, with 
 forty or more joints of varying thickness, to which are attached lengthened, jointed 
 tentacles. Interior of the pelvis disk-like or concave, exhibiting a central pit. (JZoore.) 
 
 Obs. Two specimens of this fine and interesting species are from the Mitchell 
 Downs, on the Amby River; and it is seen by the numerous arms that pass through the 
 block of limestone that a whole colony of them must have been present. One of the 
 specimens is lying on its side (exhibiting the base of the pelvis with its columnar 
 articulation), whilst three arms, with the bases of two others, are exhibited. The second 
 specimen shows the interior of the pelvis, and has arms flattened out. Each arm, above 
 the scapule, appears to have been about six inches in length. In a block from 
 Wollumbilla a portion of a column, with ninety-five regular joints, is present, of 
 
 
 
 *Emend, P. H, Carpenter, 
 
440 
 
 probably the same species. Unfortunately, some of the connecting joints of the arms 
 have been washed out, though the impressions are left indicating their direction. 
 (MLoore.) 
 
 The presence of Pentacrinoid remains in the Wollumbilla blocks was first 
 pointed out by Prof. McCoy,* in a collection from that locality, submitted to him by 
 the late Rev. W. B. Clarke. 
 
 My late friend, Dr. P. H. Carpenter, was kind enough to review this species, in 
 company with M. de Loriol. It became a question whether it really is a Pentacrinus, or 
 only one of the Comatule. Dr. Carpenter wrote: ‘‘ We both agree that the form had 
 better retain its generic name Pentacrinus till something mere is known about it. He 
 [M. de Loriol] is struck, as I am, by the absence of any reference to stem fragments in 
 the two blocks containing the specimens; and we both feel it to be quite possible that 
 they are Comatule. In any case there is a much larger number of joints (distichals) 
 before the first axillary of the arms than in any recent Comatule, which never have more 
 than four distichals, whilst there must have been fourteen or fifteen in P. australis. I 
 do not know of any recent Pentacrinus with more than seven, though it may run to” 
 seventecn in the fossil species, and to twelve in Hvtr ERLE and in the recent Metacrinus. 
 But it certainly belongs to neither of the latter genera.’ 
 
 _Loc. Mitchell Downs, Amby River; and Wollumbilla (Lhe late Be W. B. 
 
 Clarke). 
 Sub-Kinedom—ANNULOSA. 
 Class—ANNELIDA. 
 Order—TUBICOLA. 
 Family—SERPU LID ZA. 
 
 Genus—SHRPULA, Linneus, 1758. 
 (Systema, Edit. x., p. 786.) 
 SERPULA INTESTINALIS, Phillips. 
 
 Serpula intestinalis, Phillips, Ill. Geol. Yorksh., 1836, Pt. i, p. 188, t. 5, f. 21. 
 PP a Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 239. 
 
 Obs. This species is recorded by the late Mr. Charles Moore without description 
 or other reference. It is characteristic of the Oxford Clay and Cornbrash. 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Class—CRUSTACEA. 
 Order—CIRRIPEDIA. 
 
 Obs. The presence of Crustacea in the Upper Mesozoic rocks of Queensland is 
 at present not definitely recorded. The only evidence of their existence lies in the 
 following passage by Mr. Moore + :— 
 
 ‘‘ When the tests of the Australian shells are occasionally broken, or casts only 
 are preserved, it may be often noticed that the interiors were covered by Polyzoa, 
 Serpule, and other parasitic animals. On the interior of Panopea are two disk-like 
 impressions with fimbriated radiating surfaces; and it was difficult to decide whether 
 they might not be flattened corals, or even Cranie. On consulting my friend, Mr. 
 Etheridge,t respecting them, he suggested that they might be the places of attachment 
 
 
 
 
 
 * Trans. R. Soc. Vict., 1865, vi., p. 44. 
 
 + Now, of course, the rediscovery of Mr. Norman Taylor’s Crustacean invalidates this statement. 
 (RE. Junr.) 
 
 + Mr. R, Etheridge, F.R.S. 
 
44.1 
 
 of Balani or some other Cirripeds ; and on examining the collection at Jermyn Street,* 
 analogous impressions were found, produced by the attachment of these shells; so that, 
 although no other traces of the shells have been found, the family may, I think, be 
 added to the list.” 
 
 Class—INSECTA. 
 Order—NEUROPTERA. 
 Family—LIBELLUIN 2. 
 
 Genus—AESCHNA, Fabricius, 1776. 
 (Gen. Insectorum, p. 147.) 
 
 AESCHNA FLINDERSENSIS, H. Woodward, P\. 20, fig. 4. 
 
 Acschna Hlindersensis, H. Woodw., Geol. Mag., 1884, i., p. 339, t. 11, f. 1. 
 
 Obs. The first Insect discovered in Australian Mesozoic rocks has been described 
 under the above name by Dr. Henry Woodward. It was found by my Colleague in 1881. 
 The remains consist of the proximal half of the posterior wing of a Libelluloid Insect, 
 and exhibit the nervures in a remarkably fine state of preservation. As preserved, the 
 portion measured twenty-five mm. in length, and nearly fifteen mm. in depth, and when 
 perfect was probably forty-five mm. in total length. Dr. Woodward remarks—“ It is 
 the posterior wing of a Neuropterous Insect of the sub-order Odonata, Fabr., and 
 perhaps referable to the sub-family Gomphine, one genus of which, Austrogomphus, de 
 Selys, having five species, is characteristic of Australia and Tasmania.” 
 
 It is very closely allied to forms met with in the Lower Secondary rocks of 
 England—viz., the Purbeck Beds of Dorsetshire. 
 
 Loc. Flinders River, seven miles above Marathon Station (R. L. Jack). Since 
 the discovery of the above, Mr, J. H. Simmonds has found Insect remains in the Ipswich 
 Coal Measures. 
 
 Sub-Kingdom—MOLLUSCA. 
 
 Section—MOLLUSCOIDA, 
 Class—PoLyzoa. 
 Order—GYMNOLEMATA. 
 
 Family—ESCHARIDZ. 
 
 Genus—LEPRALTIA, Johnston, 1838. 
 (Hist. Brit. Zoophytes, p. 277.) 
 
 Lepratra ? oorrrica, Moore, Pl. 20, figs. 5 and 6. 
 Lepralia oolitica, Moore, Quart. Journ. Geol. Soc., 1870, xxvii., p. 248, t. 17, f. 2. 
 
 Sp. Char. Cells long, cylindrical, base soon becoming immersed, so as to 
 resemble Tubulipora or Diastopora. (Moore.) 
 
 Obs. Prof. G. Busk, who examined the species, remarked ‘that he had not 
 before noticed it, and that it did not occur in a series (Tertiary) he had examined from 
 Mount Gambier. The genus has not hitherto been found lower than the Cretaceous 
 Period. It occurs not unfrequently on the exteriors of the Wollumbilla fossils. 
 (Moore.) 
 
 * The Museum of Practical Geology, Jermyn Street, London. (RZ. Junr.) 
 
 
 
 
 
442, 
 
 On the subject of the Class Polyzoa generally, Moore made the following 
 remarks :—“ It is not improbable that this group may be numerously represented, as 
 there are frequent indications of Polyzoa; but the worn condition of many of the 
 shells to which they are attached is unfavourable to their preservation. On a cast of a 
 Cytherea from the Maranoa River numerous reticulated impressions show that its 
 interior was almost covered with them.” 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 Class— BRACHIOPODA. 
 
 Order—TRETENTERATA, 
 Family—TEREBRATU LID Z. 
 
 Genus—TEREBRATELLA, D Orbigny, 1847. 
 (Comptes Rendus, xxv., p. 269.) 
 
 TEREBRATELLA Dayripsoni1, Moore, Pl. 20, figs. 7 and 8. 
 Terebratella Davidsonii, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 245, t. 10, f. 1 and 2. 
 
 Sp. Char. Shell rather large, transversely ovate or subtrigonal, slightly convex ; 
 beak truncated; ventral area extended and slightly depressed below a lengthened, 
 slightly rounded hinge-line. The surface of the valves exhibits distinct but very 
 minute punctations, and possesses wide concentric bands, on which are regular but 
 much finer lines of growth; these are crossed by numerous radiating striz, which, 
 towards the margins of the folds, give the shell a fimbriated appearance, very fine plice 
 being visible on the whole of the surface. The larger or dorsal valve possesses a wide 
 mesial fold, with a corresponding sinus on the ventral valve. (Moore.) 
 
 Obs. Three examples of this very pretty species occur, but only one is free from 
 the matrix and tolerably perfect, and, to all appearance, belonging to Zerebratella, 
 under which genus (in the absence of internal structure) it is placed. It is the largest 
 of the Australian Brachiopoda, and I have named it Z. Davidsonii, after the Paleonto- 
 logist who has spent a life in the elucidation of this important group. (Moore.) In - 
 another specimen, collected by Mr. Sweet, the fold is very flat, and hardly perceptible. 
 
 Loe. Wollumbilla (The late Rev. W. B. Clarke; G. Sweet—Colln. Sweet, 
 Melbourne). 
 
 Family—THECIDEID. 
 Genus—ARGIOPE, Deslonchamps, 1842. 
 
 (Mém. Soc. Linn, Normandie, vii., p. ix.) 
 
 ARGIOPE P WOLLUMBILLANSIS, Moore, Pl. 20, figs. 9-11. 
 Argiope wollumbillensis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 243, t. 10, f. 3-5. 
 
 Sp. Char. Shell compressed, transverse ; hinge-line extending the entire length 
 of the shell; umbones depressed ; ventral area extended; deltidium narrow, triangular ; 
 exterior of the valves covered with coarse rounded striew, which are broken at the 
 concentric lines of growth, where they are seen to be hollow, and were probably 
 continued in spines over the folds of the shell; exterior of dorsal valve abruptly keeled, 
 the lines of growth crossing, which give the keel a comb-like appearance; interior of 
 the dorsal valve with a sinus, which terminates at the front of the shell in a deep fold, 
 and it possesses teeth-sockets, cardinal process, and distinetly raised crural plates; 
 ventral valve, in its younger state, rather flat, but becomes concave and closely fitting 
 
443 
 
 to the dorsal valve ; it possesses a deep sinus corresponding to the depression in the 
 interior of the large valves; edges of the shell closely fitting ; internal loop not known. 
 Shell structure very finely punctate. (JZoore.) 
 
 Obs. This interesting shell is found with the Pwrisiphonia and other remains at 
 Wollumbilla, and as there are evidences of several more or less perfect examples in the 
 block, it must be an abundant shell. It belongs to the group originally arranged by 
 Dr. E. Deslonchamps under dArgiope, of which he described three species from the 
 Lias, but which in his “ Palaeontologie Francaise” he subsequently removed to 
 Terebratula. Having found the same species at Whatley, and referred them to Argiope, 
 I think it convenient still to retain them in this group, though ultimately it is probable 
 they may have to be separated from it and constituted a sub-genus. At present little is 
 known of their loops or internal characters. The Australian examples are more 
 regularly striate than the European Liassie species. Where the strie on the <A. 
 wollumbillensis are occasionally abraded, a canal is visible, which leads me to suspect 
 they were originally hollow, and probably continued in spines beyond the shell, like those 
 on Athyris or Spirifera rostrata. In its outer form this shell very much resembles 
 some of the Strophomenide. (Moore.) 
 
 In another portion of his Paper Mr. Moore again remarked—‘ The peculiar 
 form of these shells, their long hinge-lines, compressed valves, and finely folded or 
 plicated exteriors, even in ignorance of the internal form of the loop, are, I think, 
 sufficient to justify their arrangement eventually under a new genus or sub-genus.” 
 
 In Mr. Sweet’s example the fold and sinus are very marked features. The 
 exterior of the shell was rugged. 
 
 Loe. Wollumbilla (Lhe late Rev. W. B. Clarke; G. Sweet—Colln. Sweet, 
 Melbourne). 
 
 ARGIOPE? PuNcTATA, Moore, Pl. 20, fig. 12. 
 Argiope punctata, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 244, t, 10, f. 6. 
 
 Sp. Char. Shell small, transversely ovate; dorsal valve flattened or slightly 
 convex; margins regularly rounded; surface of valve with bifurcating longitudinal 
 strie, which at the front are thirty in number.. (JLoore.) 
 
 Obs. This shell clearly indicates the presence of a second species of the group. 
 Only one valve is known, and this is not perfect. The strie are much more distant, 
 and stand up in sharp ridges, and the punctations are much coarser and fewer than on 
 the A. wollumbillensis. In these respects the species approaches nearer to the French 
 and English examples. The specimen is attached to the surface of a Serpula intestinalis. 
 (Moore.) 
 
 Loc. Wollumbiila (Lhe late Rev. W. B. Clarke). 
 
 Family—RHYNCHONELLID. 
 Genus—RHYNCHONELLA, Fischer, 1809. 
 
 (Notice Foss. Gouv. Moscou, p. 35.) 
 
 RuyYNCHONELLA RUSTICA, Moore, Pl. 20, fig. 18. 
 Rhynchonella rustica, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 245, t. 10, f. 7-9. 
 
 Sp. Char. Shell variable, usually wider than long, beak acute; when young com- 
 pressed, with both valves slightly convex, without sinus, and margins rounded ; with age 
 the shell is furnished with a broad sinus in the ventral, with a corresponding convexity 
 or mesial fold in the dorsal valve ; surface covered with strie, from twenty to twenty-five 
 in number, which in the adult shell are somewhat wavy or irregular. (JLoore.) 
 
444s 
 
 Obs. With age the dorsal valve becomes very convex, and the frontal margin 
 considerably thickened. It approaches most closely to the &. concinna of the Great 
 Oolite and Bradford Clay, but in its general aspect it is a coarser shell, and the 
 plicee are more irregular. I have seen about twenty examples, so that it must be very 
 abundant. In the hollows of the strie are occasionally Polyzoa and attached 
 Foraminifera. (JZoore.) 
 
 Loc, Wollumbilla District (Lhe late Rev. W. B. Clarke). 
 
 RHYNCHONELLA SOLITARTIA, Afoore, Pl. 20, fig. 19. 
 Rhynchonella solitaria, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 245, t. 10, f. 10. 
 
 Sp. Char. Shell wider than long; ventral valve with broad mesial sinus, in 
 which are four widely spreading coste, with a single lateral costa on either side of 
 the sinus. ‘Towards the umbo the shell is smooth, and without appearance of coste. 
 (Moore.) 
 Obs. Only a single specimen of a ventral valve of this species occurred in one of 
 the Wollumbilla blocks and it was not quite perfect. 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 Order—CLISTENTERATA. 
 Family—DISCINIDA. 
 
 Genus—DISCINA, Lamarck, 1819. 
 (Hist. Nat. Anim. sans Verteéb. vi., Pt. 1, p. 236.) 
 
 Disctna aprcats, Moore, Pl. 20, fig. 15. 
 Discina apicalis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, p. 244, t. 10, f. 18. 
 
 Sp. Char. Shell small, round, or slightly ovate; apex very acute, almost 
 central, or inclined to anterior end; shell-structure thin, with faint concentric lines 
 of growth. (Moore.) 
 
 Obs. Only a single, somewhat imperfect, example of this shell was seen. Its 
 chief peculiarity appears to be its very high and conical figure in proportion to its size. 
 (IMoore.) 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Family—LINGULID. 
 
 Genus—LINGULA, Bruguiére, 1878. 
 (Encyclop. Methodique, i., Pl, 250, f. 1.) 
 
 Linauta ovatis, J. Sowerby, Pl. 20, fig. 14. 
 
 Lingula ovalis, J. Sby., Min. Con. i., p. 56, t. 19, f. 4. 
 ry. 35 Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. 2, pp. 236 and 240. 
 
 Obs. The only species to be recognised amongst the Wollumbilla fossils is the 
 Lingula oralis of the Kimmeridge Clay, or the Z. subovalis of the Lower Greensand, 
 which names probably refer to the same species. This shell is most abundant, as many 
 as fifteen examples being visible on the surfaces of a block only two or three inches 
 square. Its presence assists in uniting the faune in several of the blocks which contain 
 nothing else in common. (J/oore.) 
 
 It is very questionable if this be the species figured by Davidson under this 
 name. ‘Tate has adopted for it the name of LZ. subovalis.* 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 
 
 
 
 * Proc. Austr. Assoc. Adv. Sci. for 1838 [1889], i, p. 230. 
 
 — & 
 
445 
 Section—MOLLUSCA VERA, 
 Class—PELECYPODA. 
 
 Order—OSTRACEA. 
 Family—OSTREIDZ. 
 
 Genus—OSTREA, Linneus, 1758. 
 (Systema, Ed. x., p. 696.) 
 
 OsTREA VESICULOSA, J. Sowerby, sp., Pl. 21, figs. 1-3. 
 
 Gryphea vesiculosa, J. Sby., Min. Con., 1822, iv., p. 93, t. 369. 
 Ostrea vesiculosa, Coquand, Mon. Ostrea, 1869, p. 152, Atlas, t. 59, f. 4-7. 
 ¥ y Pictet and Campiche, Descrip. Foss. Terr. Crét. Env. St. Croix, 1871, 4e Pt., p. 311, 
 t. 194, f. 1-6. 
 
 Obs. Three individuals of this characteristic and widely distributed shell have 
 been obtained in Queensland. They correspond in general characters with the excellent 
 figures by MM, Pictet and Campiche, of their specimens from the Upper Gault of 
 St. Croix. ; 
 
 Loe. Gypsum Mine, Chollarton (Hon. A. C. Gregory). 
 
 Family—PECTINID &. 
 Genus—PECTEN, O. F. Miller, 1776. 
 
 (Zool. Danicz Prod., p. xxxi.) 
 
 Precten Moore, sp. nov., Pl. 21, fig. 20. 
 Pecten fimbriatus, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 248, t. 11, f. 8. 
 
 ‘Sp. Char. Shell rather convex, with numerous longitudinal slightly nodulated 
 coste at the front of the shell, and, continuing to about the middle, where they die out, 
 are faint intermediate strie. These are crossed by regular concentric fimbriated striz, 
 which in the interspaces are produced beyond the shell. 
 
 Obs. The name assigned to this species by Mr. Moore was preoccupied by Philippi* 
 for a Sicilian Tertiary species. Under these circumstances, the foregoing designation 
 may be accepted in its place, with the view of avoiding confusion. 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 PECTEN HQUILINEATUS, Moore, Pl. 21, fig. 10 (? fig. 8). 
 Pecten? cequilineatus, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 248, t. 11, f. 11. 
 
 Sp. Char. Shell ovately orbicular, moderately convex; surface covered with 
 numerous raised divergent longitudinal striw#, crossed by about the same number of 
 equally raised concentric cost, which narrow towards the apex, where, decussating the 
 longitudinal strize, they present small folds or punctate-looking bosses; interstitial 
 spaces smooth, auricles large, unequal. (JZoore.) 
 
 Obs. This shell approaches nearest in ornamentation to the P. retiferus of the 
 Great Oolite, but it has a much larger number of concentric coste, and is much 
 more delicately marked than that shell. Several ill-preserved valves have been observed 
 in the various collections examined, which may perhaps be referred to this species. A 
 specimen of this description is figured (PI. 21, fig. 8). 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). ? Aramac (PI. 21, fig 8). 
 
 
 
 
 
 * Enum, Moll, Siciliz, 1844, ii., p. 61. 
 
446 
 
 Pecren soctatis, Moore, Pl. 21, figs. 6, 7 (2 5 and 9). 
 
 Pecten socialis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 248, t. 11, f. 10. 
 [Compare Pecten psila, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., p. 239.] 
 
 Sp. Char. Shell suborbicular, small, both valves apparently alike, moderately 
 convex, margins rounded. Dorsal margin short, shortest on the anterior side. Umbones 
 rather gibbous, pointed; ears small, triangular, flattened, the anterior the smaller of 
 the two, apparently unornamented; anterior and posterior slopes well marked. 
 Surface with very regular radiately curved stria, with four or five strong concentric 
 undulations on the umbonal region.” 
 
 Obs. The late Mr. Tenison Woods suggested that his Pecten psila might be this 
 species, and Prof. Tate has adopted * this view, but if the ears of Woods’ species are, 
 as he describes them, radiately ribbed, the two shells cannot be identical. The curved 
 radiating and very fine coste place P. socialis near the genus Camptonectes, Agassiz, but 
 I have not seen any evidence of the existence of the intercostal puncte. It reaches 
 as much as one inchin length by a half-inch in breadth, a shell of this size being in the 
 cabinet of Mr. George Sweet, and the er ti figured by Moore seems to have been of 
 similar dimensions. 
 
 In general appearance P. socialis would also seem to fall within Meek’s genus 
 Syncyclonema,t which was proposed for smooth compressed Pectens of Cretaceous and 
 Jurassic rocks, such as “cannot be properly included in the genus Pecten as restricted 
 to such forms as as P. maximus.’ It is a compressed, nearly equivalve closed genus, 
 with a short hinge-line, small ears, and no definite byssal smus. Mr. Moore made the 
 following remarks on his Wollumbilla specimen :—‘‘ The external ornamentation of 
 this shell is not well preserved; but it appears to have been nearly smooth, without 
 visible concentric striz, but with depressed radiating ribs. In general form it is not 
 unlike P. rigidus.{ It is one of the most abundant shells in the boulders from 
 Wollumbilla, many specimens of all ages appearing on their fractured surfaces.” 
 
 In Pl. 21, fig. 5, a very small, imperfect, and apparently quite smooth Pecten 
 is figured, but without other distinctive features than its form. The interior of the 
 valve only is seen. The posterior wing was very small, and obliquely rectangular, 
 the anterior somewhat larger, with a slight byssal notch below it. The hinge-line 
 was straight. This little fossil is perhaps related to the present species. 
 
 Loe. Wollumbilla (The late Rev. W. B. Clarke; G. Sweet—Colln. Sweet, 
 Melbourne) ; Walsh River (Hon. A. C. Gregory); Pl. 21, fig. 5, Mitchell Railway 
 Station (J. Falconer). 
 
 PEcTEN, sp. ind., Pl. 21, figs. 7 and 9. 
 
 Obs. A small and apparently common Pecten, of which the exterior has not 
 been seen, in some of its characters resembles P. socialis, but departs from it in the 
 relative size of the more or less flattened ears. The shells are suborbicular, with square 
 flattened ears and a shallow triangular cartilage pit. The interior surface is smooth, 
 but the shell is thin enough to show radiating strie, which become stronger towards the 
 ventral and lateral margins. They have much the appearance of the punctured radiations 
 seen in the genus Campfonectes, and divaricate rather than radiate in a similar 
 manner. The body of the shell appears to bear a series of concentric lamine (Pl. 21, 
 fig. 7). The points mentioned are clearly important features of the species, and it is 
 
 
 
 * Proc. Austr. Assoc. Adv. Sci. for 1888 [1889], i., p. 230. 
 
 + Smithsonian Check-list of N. American Cret. Foss., 1864, p. 7; also Report U. S, Geol. Survey, 
 Territories, 1876, ix., p. 26. 
 
 tJ. Sowerby, Min. Con., iii., p. 5, t. 205. 
 
44,7 
 
 to be regretted that no exteriors have been seen. There is a general resemblance to 
 Moore’s P. socials, but the details of the latter are so little known that a satisfactory 
 comparison cannot be made. 
 
 Loc. Aramac (Lhe late J. Smith); Rockwood Station, Landsborough River 
 (R. L. Jack). | 
 
 Genus—AMUSIUM, Klein, 1758. 
 (Tent. Meth, Ostr.) 
 
 AMuUSIUM, sp. ind., Pl. 21, figs. 4 and 4a. 
 » [Compare Amusium sulcatellum, Stoliczka, Pal. Indica, 1871, iii., Pts. 9-13, p. 436, t. 31, figs. 12, 12a, and 17.] 
 
 Obs. We have but the ears and umbonal portion of a single valve to represent 
 this genus. It has a general resemblance to the above species, but the apical angle 
 differs. The hinge-line is not quite horizontal, but has an inclination to an upward 
 deflection after the manner of the genus Hnfolium. The surface of the valve is a good 
 deal decorticated, but there are traces of fine regular concentric lines, as shown in the 
 enlarged figure. The umbo was small and acute. 
 
 Loe. Rockwood Station, Landsborough River (2. L. Jack). 
 
 Family—LIMIDZ. 
 
 Genus—LIMA, Bruguiére, 1789. 
 (Tab. Encycl. Méthod., Pl. 206.) 
 
 Lima Gorpont, Woore, Pl. 24, fig. 16. 
 Lima Gordoni, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 247, t. 12, f. 4. 
 
 Sp. Char. Shell ovately oblong, inequilateral, oblique, thin, with about fifteen 
 to seventeen rounded costs, which become obsolete on the posterior side, and with 
 many concentric close-set but distinct lines of growth; hinge-line narrow and straight, 
 posterior side rounded, anterior oblique ; ventral margin rounded. (JLoore.) 
 
 Obs. Casts of this species are stated to be common. Jn critically examining 
 Lima Gordoni, comparison should be made with Lima wacoensis, F. Roemer,* from the 
 Chalk of Texas, which is very close to the present species, and appears to be intermediate 
 between it and Lima Randsi. In the Texan fossil the ears are small and plain without 
 coste, whilst the coste on the body of the shell are simple with very few exceptions. 
 
 Another species to which the present is allied is Zima alternans, F. A. Roemer,t 
 of the North German Oolite, but the ribs are less in number than in the former. 
 Amongst British species Zima Gordoni is related to Lima semicireularis, Goldf., and 
 Lima duplicata, Sby. The outline is similar, but both species have more numerous ribs, 
 
 and much too close together for our species. 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 Lima ? BRAAMBURIENSIS (Sby.), Phillips ?, Pl. 21, fig. 12. 
 Avicula braamburiensis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 240, t. 11, f. 5. 
 
 Obs. Mr. Moore figured a fragment of a shell under the above name, and it is 
 to be presumed that when using it he had in view the species so named at various times 
 by Sowerby or Phillips. No description was given, but it appears absolutely certain 
 that the Australian shell figured by Moore is not the species he imagined it to be. 
 
 
 
 * Kreidebild. Texas, 1852, p. 68, t. 8, f. 7a and 6. 
 + Verst, Nord, Ool.-Gebirges, 1836, t. 12, f. 10, 
 
44.8 
 
 Nor is it at all certain what it may be, and I quite agree with an opinion expressed by 
 Prof. Ralph Tate, at a late meeting of the Australian Association for the Advancement 
 of Science,* that it is impossible to arrive at a definite solution of this shell’s identity. 
 
 Avicula braamburiensis, Phill., is a much more oblique species than that repre- 
 sented in Moore’s figure, and agrees much better with our figure of Lima Randsi (P1. 21, 
 fig. 13), but the coste of the former are finer and more numerous. 
 
 Prof. Tate suggested Pecten as a genus for this fragment, and it is quite possible 
 he may be right ; but as the figure appears to show some degree of obliquity I have placed 
 it provisionally in Lima. 
 
 Loe. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Lima ? Muutistriata, Moore, Pl. 24, fig. 17. 
 Lima multistriata, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 248, t. 12, f. 5. 
 
 Sp. Char. Shell very convex, oblique; ears very small; hinge-border very 
 narrow; surface with about forty depressed rounded coste, with narrow interstitial 
 spaces. (Moore.) 
 
 Obs. This species can only be regarded as a very unsatisfactory one from the 
 state of preservation of the original specimen. This is stated by Mr. Moore to be 
 ‘somewhat abraded,’ and with the ventral margin incomplete. I much question if an 
 identification could be effected by means of the description and figure. 
 
 The name Lima multistriata had, according to Giimbel, been already applied by 
 Geinitz to a species of the present genus. 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Order—MYTILACEA. 
 Family—A VICULID. 
 
 Genus—OXYTOMA, Meek, 1864. 
 (Smithsonian Check-list N. American Cret. Foss., p. 29.) 
 
 OXYTOMA ROCKWOODENSIS, sp. nov., Pl. 24, fig. 15. 
 
 Sp. Char. Shell (left valve) subrotundate, very convex and tumid, alate pos- 
 teriorly,and moreorlessoblique. Hinge-line straight, but not equal to the width of the shell ; 
 ventral margin obliquely rounded. Anterior ear, or wing, not well preserved, butapparently 
 not distinctly separable from the anterior end of the shell; posterior wing moderately 
 large, flattened, abruptly cut off from the body of the shell by a marked posterior slope. 
 Umbo depressed but evenly convex, inrolled but not greatly overhanging the hinge- 
 line. Surface with fourteen or fifteen strong, simple, non-spinous, distinet radiating 
 cost, the interspaces flattened, or even a little concave, occasionally bearing a smaller 
 interpolated rib, but quite distinct from the larger ones, the interspaces being crossed 
 by almost microscopic wavings ; the posterior wing bears not more than one or two coste. 
 
 Obs. The present species is evidently congeneric, so far as the characters of the 
 left valve go, with those bivalves for which the late Mr. F. B. Meek proposed the genus 
 Oxytoma—viz., Avicula Miinstert, Bronn ; A. echinata, Miinster; and Avicula costata, Sby. 
 These remarks are, of course, made on the supposition that the flat valve will correspond 
 with those of the foregoing species; at present, however, it is unknown. 
 
 O. rockwoodensis also stands in the same relation to Stoliczka’s Psewdomonotis 
 semiglobosa,t and is even closely related specifically. But the Indian shell is not a 
 
 * Proc. Austr. Assoc. Adv. Sci. for 1888 [1889], i., p. 229. 
 + Pal, Indica (Cretaceous Fauna), 1871, iii., Pts, 5-8, p, 402, t. 26, f. 1. 
 
449 
 
 Pseudomonotis, and does not agree withthe peculiar Bivalve for which Beyrich* instituted 
 the latter genus—viz., Monotis speluncaria, Schl. From Stoliczka’s species, O. rockwood- 
 ensis differs in its much greater size, larger number of coste, presence of the smaller inter- 
 polated ones, and an increased convexity of the surface; nor do I think that it is in 
 any way connected with Moore’s Avicula simplex,t A. equalis (Pl. 24, fig. 3), or his 
 Arca (?) plicata (Pl. 24, fig. 5), as our shell is much too generally globose, and 
 possesses a different posterior wing, and on the whole, appears to agree better with 
 the left valve of Oxytoma than with any other genus. Of some of these supposed 
 species I have seen the types in the Bath Museum, and can only say that the species 
 are founded on wretchedly small and most unsatisfactory material. Oxytoma is a 
 typical Avicula, but more inequivalve, with a very deeply cut byssal sinus close under 
 the anterior auricle of the right valve; the left valve, on the other hand, should be 
 convex, or even globose, sharply ribbed, or echinated, and with a somewhat deeply cut 
 posterior wing. O. rockwoodensis is no more convex about the umbonal region than 
 the Oolitic Oxytoma echinata, Sby. 
 
 Loc. Rockwood Station, Landsborough River (2. LZ. Jack); Aramac (The 
 late James Smith). 
 
 Oxytoma.? stmpLEXx, Moore, Pl. 24, figs. 2-5. 
 
 Avicula simplex, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 247, t. 11, f. 3 (? f. 4). 
 »,  cequatis, Moore, loc. cit., t. 11, f. 4 (? f. 3). 
 Arca plicata, Moore, loc. cit., p. 249, t. 12, f. 6. 
 
 Sp. Char. Shell small, very inequilateral. Left valve convex, thickened about the 
 umbonal region ; right valve flattened, plain. In the left valve the cardinal margin or 
 hinge line straight, long. Posterior wing very extended; anterior wing small. Surface 
 with seven or eight sharp, well-separated radiating coste and a few concentric lamine. 
 
 Obs. In describing Avicula simplex and A. e@equalis, Mr. Moore would 
 appear to have transposed the numbers of the figures representing these fossils in the 
 eleventh plate. His definition of A. simplex corresponds not to fig. 3, as stated, but 
 to fig. 4, and vice versd; the description of 4A. equalis is applicable to the latter 
 figure, and not to the former. The types of these so-called species are in the Bath 
 Museum, and have been examined by me. Both are very small shells, and the original 
 of Moore’s fig. 5 (A. simplex as it should be) is fairly well represented. But the type 
 of his fig. 3 (A. @qualis in reality) is a very obscure specimen, and is more correctly 
 represented in our Pl. 24, fig. 2. It is the opposite valve to Moore’s fig. 4, and may 
 quite well represent its right valve; in fact, if this is so, it will fairly well accord with 
 what takes place in other species of Oxytoma. 
 
 I cannot see on what possible grounds Moore separated from the foregoing a 
 small shell termed by him Arca plicata. There is no evidence of its Arca-affinity; but 
 having the entire outward appearance of O.? simplex, I have united it with the latter. 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke); Minmi, near Roma (f#. LZ. 
 Jack). 
 
 Genus—PSEUDAVICULA, gen. nov. 
 
 Gen. Char. Shell in general outline meleagriniform, but devoid of an anterior 
 wing or ear. Valves compressed, closed, nacreous within, bi-convex, inequilateral. 
 Cardinal margin thin, no area, or hinge teeth, but probably with a small ligament. 
 Posterior wing moderately developed, but with little or no emargination. Adductor 
 muscular scars subcentral, of medium size. 
 
 
 
 
 
 * Zeitsch. Deutschen Geol. Gesellsch., 1862, xiv., p. 10, 
 + Quart. Journ, Geol. Soc., 1870, xxvi., t. 11, f. 3. 
 
450 
 
 Obs. This genus is proposed to include two shells described by Mr. Moore as 
 referable to Zucina, the characters of which are but imperfectly known to me; never- 
 theless, they are sufficiently clear to show that they cannot be referred to a so-called 
 Dimyarian genus, but in all probability partake more of the nature of the Aviculide. 
 The genus must, therefore, be looked upon as, to some extent, provisional. 
 
 Although I never understood Moore’s reference of his species to Lucina, it was 
 not until Mr. H. Y. L. Brown forwarded a series of specimens to the Natural History 
 Museum, London, from Coottanoonna, in South Australia, that I was able to satisfy 
 myself that Lucina anomala and L.? australis were not Lucine, but a Monomyarian 
 shell. 
 
 Moore described both his species as nacreous, and this should have at once -been 
 sufficient to exclude these shells from the Lucinide. The separation into two species 
 depended only on the presence in one of finer coste, and a less extended anterior hinge- 
 line. The condition of the surface costs is perhaps due to preservation; and as regards 
 the “less extended anterior hinge-line,’ the extended portion is posterior and not 
 anterior, and the degree in this particular case is again to some extent a question of 
 preservation. When perfect the shells are decidedly inequilateral, and this at once 
 does away with the mesial beaks. The only remaining Luwcina character is the lunule 
 said to exist in Z. anomala, but I have failed to detect such a structure in the specimens 
 examined by me. 
 
 The point of view here advocated is supported by the nacreous character of the shell, 
 the absence of hinge teeth, and the presence of a large adductor muscle, which is shown 
 in one of Mr. Brown’s specimens... The essential points in the genus, in addition to the 
 general shape, are the absence of an anterior ear, the anterior margin being 
 regularly and gently rounded; small byssal sinus; and the simplicity of the hinge 
 mechanism. JI am not acquainted with the latter as thoroughly as I could wish, 
 but from the appearance of the cardinal margin in Pl. 24, fig. 12, the absence 
 of teeth can safely be surmised. In all probability the valves were held together by 
 a small external ligament and internal cartilage, placed in a groove, visible in the 
 figure, as described by Hudleston. It is hardly necessary to point out that these shells 
 are quite distinct from Avicula, as typified by A. hirwndo, Linn. 
 
 Type—Lucina anomala, Moore. 
 
 PSEUDAVICULA ANOMALA, Moore, sp., Pl. 24, figs. 6, 8, 11. 
 Lucina anomala, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 251, t. 14, f. 4. 
 
 Sp. Char. Shell suborbicular, generally compressed, thin, posteriorly alate ; valves 
 slightly convex, flattened towards the margins. Dorsal margin short, straight on the posterior 
 side ; anterior margin rounded below, abruptly cut off and obliquely rounded above; pos- 
 terior margin obliquely sub-truncate, entire posterior wing flattened, the angle rounded. 
 Umbones small but prominent; byssal sinus small, distinct. Sculpture consisting of a 
 large number of very fine regular radiating cost, becoming parallel to the dorsal margin 
 on the wing, crossed by equally delicate concentric lines, broken up into broad bands 
 or lamin, giving rise to flattened quadrangular spaces, the points of intersection 
 becoming delicately serrate. 
 
 Obs. This species invariably occurs in large numbers matted and compressed, 
 always presenting the same physical appearance, and invariably of the same size, 
 seldom exceeding eleven-sixteenths of an inch in transverse measurement. I at one 
 time took this and the following species to be one, but the constant uniformity in size 
 and much sharper surface sculpture of the present shell compel me to retain them 
 separately—at any rate, provisionally so. Moore speaks of his Lucina ? australis as 
 
451 
 
 larger than the L. anomala, a remark which will bear out the identification now made, 
 but I opine that Moore’s figure of the last-named species is magnified, as I have not met 
 with a specimen so large, Psewdavicula anomala is a pretty shell, and, from the quantity 
 in which it occurs and its glistening appearance, forms an attractive specimen in any 
 cabinet. I do not find any difference in the size ofthe valves, so it was probably 
 equivalve, as Moore says. 
 
 Loc. and Horizon. Wollumbilla (The late Rev. W. B. Clarke ; G. Sweet—Colln. 
 Sweet, Melbourne) ; Maranoa River, half a mile above Mitchell Railway Station (2. L. 
 Jack) ; Maranoa (@. Sweet—Colln. Sweet, Melbourne). 
 
 PSEUDAVICULA AUSTRALIS, Moore, sp., Pl. 24, figs. 7, 9, 10, 12, and 13. 
 
 Lucina ? australis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 251, t. 14, f. 5. 
 Avicula orbicularis, Hudleston, Geol. Mag., 1884, i., p. 341, t. 11, f. 10. 
 Pseudavicula anomala (pars.), Hudleston, Geol. Mag., 1890, vii. (3), p. 244. 
 
 Sp. Char. Shell generally meleagriniform in outline, unequally orbicular, and 
 possessing but little convexity of valves. Dorsal margin short, straight on the posterior 
 side, involute on the anterior side, with a byssal sinus of moderate size; anterior 
 margin obliquely and sharply cut off above, rounded below; ventral margin fully 
 rounded ; posterior margin sub-truncate, obliquely inclined upwards; posterior wing 
 small, rather flattened, angle rounded. Umbones slightly more anterior than posterior, 
 small and sharp, but depressed. Adductor sear almost central, large, longitudinally 
 elongated and bearing crescentic impressions. Surface sculpture as in the preceding 
 species, but less sharply defined. 
 
 Obs. P. australis is decidedly larger than that I take to be P. anomala, 
 and although the sculpture is of the same type, it is never, so far as my experience 
 goes, so sharp and regular. The test of P. australis must have been very thin, as it is 
 seldom actually preserved. The only hinge structure so far made out is a simple 
 involution of the dorsal magin (Pl. 24, fig. 12) in which the ligament was placed. 
 
 The shell figured by Mr. Hudleston as Avicula orbicularis is without doubt 
 identical with the present species. I am convinced of this after comparing the type at 
 the Natural History Museum with numerous other specimens collected by Mr. H. Y. L. 
 Brown in South Australia. 
 
 Prof. Ralph Tate would appear to refer * Hudleston’s Avicula orbicularis to 
 Maccoyella Barklyi, Moore; ut in so doing he is clearly wrong, their structure being 
 quite distinct. 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke ; G. Sweet—Colln. Sweet, Mel- 
 bourne); Maranoa River (G. Sweet—Colln. Sweet, Melbourne); Coottanoonna, S- 
 Australia (H. ¥. L. Brown—Colln. Brit. Mus., London); Lake Eyre District (Prof. 
 R. Tate—Colln. Adelaide University). 
 
 Genus—MACCOY ELLA, gen. nov. 
 
 Gen. Char. Shell oval, or orbicular, inequivalve, inequilateral, slightly produced 
 obliquely at times, and with a flattened, sub-truncate, or slightly emarginate posterior 
 end in both valves. Valves plano-convex, slightly concavo-convex, or more or less 
 bi-convex. Anterior end sometimes more or less lobate. Cardinal margin straight 
 on the posterior, but oblique on the anterior side. Hinge much thickened and 
 strongly grooved for cartilage attachment in both valves; in the right or generally 
 non-convex valve the hinge is strongly inflected or folded inwards at or anterior 
 to the umbo, producing a deep, narrow, and obliquely directed byssal sinus; in 
 -=- ee Sy 
 
 
 
 * Proc. Austr, Assoc, Ady, Sci. for 1888 [1889], i., p, 230. 
 
4.52 
 
 the left or convex valve the hinge area is shorter, wider, and triangular under the 
 umbo, and is divided more or less distinctly into two ill-defined cartilage concavities, 
 separated by a rather prominent ridge; the folding of the hinge of the right valve gives 
 to it the appearance of possessing a deeply separated and lobate small anterior ear. In 
 the left valve the anterior ear is not defined from the body of the shell, but is repre- 
 sented by a corrugated thickening of the hinge. Adductor impression very large. 
 Surface bearing radiating cost#, more numerous on the left valve, delicate concentric 
 strie, and concentric growth-lamine, the poimts of intersection being sometimes spinose. 
 
 Obs. I have much pleasure in proposing this genus in honour of Professor Sir 
 F. McCoy, of Melbourne, taking for the type species Moore’s Avicula Barkly. 
 
 It is hardly necessary to mention that the shelis included by the late Mr. Moore 
 in Avicula do not in any way correspond to that genus, as restricted by Lamarck, and 
 typified by the well-known Avicula hirundo, Linn. In the Queensland shells there is 
 an entire absence of the narrow extended posterior wing, deeply emarginate posterior 
 end, and the small pseudo-cardinal teeth of Avicula ; but, on the other hand, there is 
 a much greater inequality of the valves and a peculiar hinge mechanism quite foreign 
 to the genus quoted. 
 
 The chief peculiarities of Maccoyeila lie in the structure of the hinges of both 
 valves. In the right valve of the type species and I. reflecta there is a broad and 
 strong area, with many longitudinal cartilage furrows, the course of which is inter- 
 rupted by a strong inward inflection, or fold of its substance, having much the 
 appearance of a small lobate ear, and in addition giving rise to a narrow but deep 
 byssal sinus. It does not, however, appear to partake of the true nature of an auricle. 
 The fold is well shown in PI. 23, figs. 6 and 7, and the false ear in Pl. 22, figs. 4 and 5, 
 and Pl. 23, fig. 2; but it will be observed that the cartilage furrows are continuous 
 along the whole length of the area (PI. 23, fig. 7). 
 
 In the convex or left valve the area is similar, but in addition somewhat 
 triangular under the umbo, and there would appear to be two depressions in which 
 thickened portions of the cartilage, or plugs, were inserted. 
 
 The umbo in the left valve is prominent, convex, and overhangs the hinge to 
 some extent, but it is not usually inrolled. In the right vaive it is insignificant. The 
 muscular impressions are only known in the type, and will be found described under 
 that species. 
 
 Avicula Barklyt, Moore, approaches more closely to Meleagrina, Lamk., especially 
 in the convexity of its valves, broad cartilage area, form of the posterior wing, deep 
 byssal sinus, and the small cleft pseudo-ear of the left valve. On tle other hand, the 
 size of the right umbo is quite unlike that of Avicula margaritifera, Linn., the Mother- 
 of-Pearl Oyster, and type of the genus Meleagrina, not to mention the inflection 
 of the cartilage area. The tumidity and prominence of the right umbo would appear 
 to indicate a relation to Oxytoma, Meck, typified by Avicula Miinsteri, Bronn, but the 
 posterior wing and byssal notch differ so widely from those of Moore’s species that 
 they can hardly be congeneric. 
 
 J am sorry to be unable to agree with so distinguished an authority as Prof. 
 R. Tate in referring the shell now under discussion to the genus Jfonotis, Bronn. 
 The latter, as represented by JL. salinaria, Bronn,* is an ovate compressed shell, almost 
 equivalve, with the beaks only slightly projecting, and in no way whatever resembling 
 Moore’s species. The same remarks apply to other allied genera, suchas Halobia, 
 Bronn, and Daonella, Mojsisovics. None of the genera previously mentioned possess 
 
 
 
 7 
 * Jahrb. fiir. Min., 1830, p. 284, t. 4, f. 1. 
 
453 
 
 the peculiar hinge structure of Avicula Barkly, so faras I have been able to ascertain. 
 There is a resemblance, however, with Psewdomonotis, Beyrich,* in the proportion of 
 the valves, deeply cleft pseudo-ear, and strong byssal sinus; but in the type, P. 
 speluncaria, there is no posterior wing, but an irregular auriculate end, without any 
 parallelinthe Queensland shells. Especially does Maccoyella approach those shells from the 
 Carboniferous Series of the Salt Range, in India, described by Dr. A. Waagen,f such as 
 Pseudomonotis garforthensis, King,t or P. kazanensis. Even Waagen’s species differ a 
 good deal from P. speluncaria, and I much question if they can be regarded as true 
 members of the genus Psewdomonotis. We are unable to discover from Waagen’s 
 remarks that the hinge structure of his shells and Avicula Barklyi, Moore, in any way 
 agree in detail. His description of P. kazanensis is as follows :—‘“ The hinge is very 
 simple. -It shows in the middle a somewhat triangular emargination, very likely for the 
 reception of a cartilage. Anteriorly to it there is a broad facet, which reaches to the 
 end of the anterior wing. Its lower margin is somewhat prominent, and: forms a kind 
 of very indistinct elongated tooth. Posteriorly to the ligamental groove the hinge-line 
 is simply thickened.” 
 
 The nearest ally of Maccoyella, so far as my researches have yet gone, is 
 undoubtedly Whitfield’s Jeleagrinella,§ typified by Avicula curta, Hall.|| The 
 resemblance lies in the general appearance of the two genera, the presence of a deeply 
 cut-off ear in the right vaive, and the thickened area of the left valve. But the 
 structure of the divided ear and hinge-line of the right valve is wholly different, as the 
 following quotation will show. Speaking of the byssal fold, Whitfield says it is 
 “either a deep channel on the external surface of the shell extending from the margin 
 to near the beak of the valve, or a simple deep straight notch separating the wing into 
 a linear process, of greater or less length, from the body of the shell.’ There is no 
 structure here corresponding to the inflection or fold of the hinge in the right valve 
 of Maccoyella, nearly central in position, whereas the byssal fold of Meleagrinella is 
 anterior. In addition to this, the inequality in the size of the shell in the two genera is 
 most marked. Under these circumstances I believe I am justified in separating 
 Moore’s shells as the types of an undescribed genus. 
 
 The whole group of species, but more especially the type, MZ. Barklyi, bear 
 in their external appearance a marked resemblance to some inequilateral forms of 
 Hinnites, such, for instance, as H. Studeri, Pictet and Roux, from the Gault of St. 
 Croix.9 ) 
 
 The number of species referable to Maccoyella is at present open to doubt. 
 Moore described the following under the name of Avicula :—Avicula Barklyt, A. reflecta, 
 A. umbonalis, A. corbiensis, A. substriata, A. simplex, and A. equalis, but the two last 
 may be at once dismissed from consideration. The late Rev. J. E. T. Woods** clearly 
 considered the whole as varieties of one species. He wrote: “ Anyone who examines 
 the series figured by Mr. Moore from Wollumbilla, including eight species, will be 
 inclined to refer them all to one, differing from each other merely in size and mode of 
 growth.’ With all due respect to this adverse opinion, it is not so easy to refer all of 
 
 
 
 * Zeitsch. deutschen Geol. Gesellsch., 1862, xiv., p. 10. 
 
 + Pal. Indica (Salt Range Fossils), Vol. i., 1881, Pt. 3, p. 276. 
 
 a) 06, C2t., 61 22, £. 2 
 
 § Mon, U.S. Geol. Survey (Powell’s), 1885, ix. (Raritan Clays and Greensand Marls of New Jersey), 
 Basie 
 
 || U. S. Geogr, Geol. Survey (Powell’s) Rocky Mountain Region (Pal. Black Hills of Dakkota), t. 3, 
 f, 20-25. 
 
 7 Pal. Suisse, 5me. Série, 4me. Pt., p. 282, t. 179, f. 1. 
 
 ** Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. 2, p. 240. 
 
454 
 
 the before-mentioned shells to one species, and rash statements of the kind quoted do 
 not tend to assist in unravelling the question. I have retained Maccoyella Barkly?, 
 M. reflecta, M. wnbonalis, M. corbiensis, and. ? substriata. 
 
 It is even possible that an additional species may exist. ‘PI. 24, fig. 1, represents 
 aright valve * devoid of the posterior wing, without cost, but possessing strong con- 
 centric lamine and the general peculiar shape and shell-structure of a Maccoyella. It 
 seems distinct from either of the other species placed in this genus. 
 
 The hinge structure of the various species of MJaccoyella, although appearing to 
 differ widely at first, is found on examination to follow a well-marked plan, and afford 
 a really excellent example of paleontological morphology, from the semi-pectinoid 
 outline and restricted and convoluted hinge of I. Barklyi and MW. reflecta to the 
 gryphea-form shape, and small area of MW. corbiensis. Between these two extremes 
 stands M. wmbonalis, acting as a connecting link. In HM. Barklyi and I. reflecta the 
 umbonal fold is thick and projecting, but short, the byssal fold on the contrary being 
 much longer and projecting inwards, with a very deep and narrow byssal sinus anterior 
 to it. The hinge is thus much broken up, and does not present the same regularity of 
 outline as seen in AL. wmbonalis and M. corbiensis. In the right valve of the first of 
 these species, being that with which I am best acquainted, the dorsal margin is long 
 and obliquely bevelled, the area comparatively flat with a decided submedian cartilage 
 depression, and the folds, umbonal and byssal, prominent, but not nearly to the same 
 extent as in the two former species. The umbonal is nearly vertical, with the larger 
 portion of the concave cartilage depression posterior to it. The byssal fold is less 
 prominent still, wherein this species departs greatly from the typical structure of 
 M. Barklyi and M. reflecta, and the byssal sinus is tolerably long but not very deep. 
 In DL. corbiensis the hinge structure least resembles that of the genus of any of its 
 species. The dorsal margin of the left valve is much arched, widening out below the 
 umbo into a rather triangular, concave, cartilage area, divided excentrically by the 
 umbonal fold, the byssal fold being obsolete. 
 
 The hinge structure of the smaller species referred to Maccoyellais unknown to me. 
 
 The structure of the test in Maccoyella is non-prismatic, and apparently laminar- 
 fibrous. Thin sections show no trace of the prismatic-cellular structure of the 
 Aviculide ; but as I cannot be certain that the actual outer layer has been examined, 
 a decision on this point must be suspended. It is probable that the interior of the 
 valves was nacreous. The surface of the best-preserved examples examined by me 
 shows a hackly-laminar appearance irrespective of the outside ornament. 
 
 The distribution of Maccoyella is very extensive. The original localities recorded 
 by Moore are Wollumbilla and Mount Corby (Rolling Downs). Species have since been 
 obtained by the Hon. A. C. Gregory at the Walsh River (Rolling Downs) ; by Messrs. 
 Jack and Rands at Maryborough (Desert Sandstone) ; probably also by the latter at 
 the Isis River (Desert Sandstone); by Messrs. Jack and Samwell at the Croydon 
 Gold Field (Desert Sandstone) ; and probably by Mr. Jack at Minmi, near Roma 
 (Rolling Downs). Numerous examples have been collected by Mr. H. Y. L. Brown 
 in the Lake Eyre District, South Australia; whilst Prof. R. Tate has recorded the 
 presence of the genus in the Peak District of the same Province. Finally, as 
 intermediate between the Queensland and South Australian localities, the late Rev. 
 J. E. T. Woods has figured examples from the Gray Ranges, on the borders of this and 
 the former Colony. 
 
 Lype—Avicula Barklyi, Moore. 
 
 
 
 
 
 *Tt was collected by my Colleague at Richmond Downs, Flinders River, from the Rolling Downs Formation. 
 
455 
 Maccorentia Barxuytr, Moore, sp. 
 
 Pl. 22, figs. 1-5; Pl. 42, figs. 4-6; ? Pl. 28, figs. 1 and 2. 
 
 Avicula Barklyi, Moore, Quart. Journ. Geol. Soc., 1870, xxviii, p. 245, t. 11, f. 1-2, 
 Streptorhynchus Davidsoni, Etheridge, Ibid., 1872, xxviii., p. 333, t. 17, f. 1. 
 Monotis Barklyi, Tate, Trans. R. Soc. 8. Australia, 1885, vii., p. 76. 
 
 Sp. Char. Shell sub-orbicular, sometimes irregularly or slightly obliquely 
 so; test thick; valves plano-convex, or slightly bi-convex ; hinge hardly as long as the 
 shell; ventral margin rounded. Posterior wing more or less flattened in the right 
 valve, and much larger than in the left, where it is sharply cut off by an umbonal 
 ridge ; posterior margin usually rounded and graduating into the ventral. Umbones 
 very unequal; in the right valve small and inconspicuous; in the left prominent and 
 blunt, projecting above the dorsal margin, but not greatly overhanging it. Scar of the 
 adductor large in the right valve, nearly central, sub-reniform in outline; a deep pit is 
 present behind the inflected portion of the cartilage area, and united to the adductor 
 scar by a series of muscular pits arranged in a semicircle. The radiating coste of the 
 left valve are strong and prominent, from nine to thirteen in number, but fewer than 
 those of the left; the posterior costa, and sometimes others, stronger and larger than the 
 others, and bearing strong projecting spines; intercostal spaces with a secondary costa 
 between every pair of primary costs; the right valve bears a largely increased number 
 of coste; in both valves are several broad concentric lamine of growth, but in the 
 right these become elevated on the anterior dorsal margin into prominent undulating 
 ridge-like folds. 
 
 Obs. Mr. Moore stated that sections of this shell were to be found in almost 
 every block of matrix from Wollumbilla examined by him, a fact I am able to confirm 
 from independent observation. It is also true that JZ. Barklyi possesses a much 
 wider geographical range than was at first contemplated by its describer. Furthermore, 
 it is one of the most important shells, from a stratigraphical point of view, met with in 
 the Upper Mesozoic Rocks of Eastern Australia. 
 
 The surface coste in I. Barklyi, although varying in individuals to some 
 extent, are characteristic, but this variability may perhaps have some relation to the 
 state of preservation of the specimens. The left valve bears from nine to twelve * or 
 even thirteen sharp, separate, and prominent ribs, usually alternating with an equal 
 number of finer secondary ribs which stop short of the umbo by some little distance. 
 The posterior wing is free of cost and separated from the body of the valve by the 
 most posterior principal costa, which takes the place of an umbonal or diagonal ridge 
 in the higher bivalves. The secondary coste are sometimes increased to two, or even 
 three, between each pair of primary, but the latter number is rare. The whole valve 
 is concentrically crossed by well-marked laminar imbrications, the points of intersection 
 with the primary coste projecting as spines (PI. 22, fig. 3; Pl. 42, figs. 4 and 5), 
 especially in young individuals; but in more: mature individuals these projections 
 become worn down, and are retained in some cases only on the last posterior, the pen- 
 ultimate, and the anti-penultimate cost. The presence of these spines gives to 
 the fossils much the appearance of the genus Plagiostoma. One peculiar fact in con- 
 nection with the concentric lamine is the manner in which they pass over the anterior 
 dorsal margin as ridge-like folds (Pl. 22, fig. 2; Pl. 23, fig. 4), and there is reason to 
 believe they are conterminous with some of the cartilage furrows of the anterior 
 area. 
 
 
 
 * In one case only six were observed. 
 
456 
 
 The right valyo i is invariably but slightly convex, so far as my own observation 
 has gone, ail the umbo insignificant. The valve is, however, traversed by a much 
 larger number of coste of both orders, but there is no appearance of the ridges on 
 the anterior dorsal margin. Both valves have the intercostal spaces concentrically 
 traversed by very fine delicate wavy lines (Pl. 22, figs. 1-3); indeed, this appears to be a 
 character common to the whole group (Pl. 23, figs. 1-3). The right valve at times 
 assumes a transversely elongated outline, giving to it a most unusually inequilateral 
 appearance. This seems to be caused by a pr agen gation or extension of the depressed 
 anterior end (PI. 22, fig. 4), and is particularly motucenbled in specimens from the Croydon 
 Gold Field. 
 
 The large adductor impression in the right valve is nearly central, and is con- 
 nected by a line of muscular points of attachment to a deep and pit-like excavation 
 under the inflection of the area. This, in casts, appears as a sharp projecting point. 
 On the anterior side of the adductor the muscular attachments become clustered, and ~ 
 are placed at some considerable distance from the anterior margin. 
 
 The resemblance of Maccoyella Barklyi to Pseudomonotis garforthensis, King, 
 has been already dwelt on. With IZ. wmbonalis, Moore, and M. corbiensis of the same 
 author, we are at present not thoroughly acquainted, but it would appear that the 
 very central position of the umbones in the former, the increased convexity in the 
 latter, and the more numerous and regular radiating coste in both may be taken as 
 points for future separation—that is, supposing these shells to be separate and valid 
 species. 
 
 Through the kindness of Mr. C. W. De Vis, I have been able to examine 
 the shell named Streptorynchus Davidsoni,* by Mr. R. Etheridge, F.R.S., which 
 formed a portion of Mr. Daintree’s Collection. I find it to be an undoubted MWae- 
 coyella, either I. reflecta, or this species, probably the latter, and is either from 
 Wollumbilla, or the Walsh River, it being rather difficult at times to distinguish the 
 matrices apart. 
 
 A rather worn specimen (PI. 23, figs. 1 and 2), is provisionally united with 
 M. Barklyi, as it appears to accord better with that species than with JZ. reflecta. The 
 shell, measuring nearly two and a-half inches square, is larger than the generality of 
 individuals of the former. It is from the Walsh River. 
 
 In Pl. 22, fig. 3, I have given an illustration of the Maryborough variety of 
 M. Barklyi, which is distinguished by the size and rugosity of the primary coste and the 
 development of the posterior spines; and it is, in addition, a smaller shell. In an 
 internal cast from this locality the costw also appear to terminate along the front 
 margin in a series of free spines. Similar features are present in the form of our shell 
 from Croydon (PI. 42, fig. 5). 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke); Walsh River (Hon. A. C. 
 Gregory); Bungeworgorai Creek, near Mount Abundance; Blythesdale Station, 
 between Wollumbilla and Roma; Maranoa River, at Mitchell+ (G. Sweet—Colln. 
 Sweet, Melbourne). In South Australia at Peak Creek (Messrs. J. S. Chandler 
 and J. Canham{); and forty-five miles south-west of Cootanoonna, Lake Eyre 
 
 (H. Y. L. Brown—Colln. Nat. Hist. Mus., London). Occurs also in the Desert 
 Sandstone. 
 
 * Quart. Journ. Geol. Soc., 1872, xxviii., p. 333, t. 17, f. 1. 
 
 + With the valves in apposition, and the best examples I have seen. 
 
 ~ Teste Tate, Trans. R. Soc. 8. Australia for 1879-80 [1880], iii., p. 179; Zbid., 1880-81 [1882], iv., 
 p. 149. 
 
— 
 
 457 
 MAccoYELLA REFLECTA, Moore, sp. 
 
 Pl. 20, figs. 1, 3, 5, 7, and 10. 
 Avicula reflecta, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 246, t. 12, f. 1. 
 »  Barklyi, var. reflecta, Ten. Woods, Proc. Linn, Soc. N. 8S. Wales, 1883, viii., Pt. 2, p. 240, t. 12, 
 . 4-6, 
 
 Sp. Char. Shell large, transversely oval; valves to some extent compressed, 
 especially on the posterior side, very inequivalve, inequilateral, plano-convex, or concavo- 
 convex. Right valve either flat, a little concave, or slightly convex in the umbonal 
 region, becoming concave and then flat towards the ventral margin; anterior dorsal 
 margin moderately obliquely inclined; posterior dorsal margin straight ; area inwardly 
 bevelled, wide, with a thickened inflection, strong cartilage furrows, and a narrow, deep, 
 and inwardly curved byssal sinus; umbo smalf and nucleus-like, posterior wing large 
 and flattened, margin roundly truneated. Left valve convex, but not strongly so, the 
 greatest convexity being in the umbonal region, thence rapidly decreasing to the ventral, 
 margin; umbo elevated, but not highly so, or gibbous; anterior folds of the area not 
 particularly coarse; posterior wing not sharply marked-off from the body of the shell 
 flattened. Surface of the right valve bearing a very large number of radiating ribs or 
 coste of nearly equal size, covering the whole valve. Left valve similarly ornamented, 
 but the cost. stronger, present on the posterior wing, and every fourth rib larger- than 
 the others. Concentric lamine of both valves widely separated ; points of intersection 
 of the laminz and coste elevated into projecting frills. Muscular impressions as in the 
 type species. 
 
 Obs. The shells that I have considered referable to Moore’s Avicula reflecta are 
 of much larger size than the preceding, Waccoyella Barklyi, and in comparison it must 
 be borne in mind that Moore’s figure was reduced one-half. In addition, the whole shell 
 is much less convex, the right valve flat, or, what is more usually the case, convex in the 
 umbonal region, becoming concave forwards. The surface costs are much more numerous, 
 and in the right valve smaller, giving to that valve a far more finely striated appearance 
 than the corresponding half of WZ. Barklyi. There is little short of forty or fifty coste on 
 the left valve of J. reflecta, and in extreme specimens perhaps even more, but, as in the 
 case of the former species, the number of secondary costs between the primary varies to 
 some extent. The principal coste do not appear to project at the points of intersection 
 of the concentric lamin, as semi-tubular spines, so far as I have been able to ascertain. 
 The convexity of the left valve in this species is fairly marked in the dorsal portion 
 of the valve ; yet, ata puint about midway between the dorsal and ventral margins, 
 the diameter of the valves, when in apposition, as ascertained from two fractured 
 examples, is only seven-eighths of an inch. 
 
 The inflection of the area of the right valve is very marked in this species, the 
 inturned portion forming a kind of plug, filling the excavated portion of the left area 
 immediately under the umbo of that valve. 
 
 The muscular impressions appear similar to those of WM. Barklyi, but are not as 
 deeply excavated. 
 
 The geographical distribution is equally wide with that of MZ. Barkly. 
 Irrespective of the Queensland localities, Mr. H. Y. L. Brown has obtained it at 
 Primrose Springs, north of Lake Eyre; specimens are in the Mining and Geological 
 Museum from Milparinka, and Dunlop Station, Darling River. 
 
 Loc. and Horizon. Wollumbilla (The late Rev. W. B. Clarke) ; Bungeworgorai 
 Creek, near Mount Abundance (G. Sweet—Colln. Sweet, Melbourne) ; Lake Eyre Basin 
 (HZ. ¥. L. Brown, and Prof. R. Tate). Occurs also in the Maryborough Beds— 
 Desert Sandstone. 
 
458 
 
 MaccoyvELia umMBonatis, Moore, sp., Pl. 22, figs. 6-7, Pl. 23, fig. 4. 
 Avicula umbonalis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 246, t. 12, f. 2 and 3. 
 
 Sp. Char. Shell large, transversely ovate, almost plano-convex, nearly equi- 
 lateral ; dorsal margin long, straight, nearly equal‘on both sides the umbones. Left 
 valve moderately convex, its umbo much produced, and incurved over the hinge-line ; 
 anterior, posterior, and ventral margins rounded, the first slightly obliquely so, especially 
 above, leaving a well-marked byssal sinus ; anterior dorsal margin much crenulated, as in 
 M. Barklyi. Right valve more or less flattened, or slightly convex. Hinge area of 
 the left valve moderately large, intersected by the two transverse folds, one 
 immediately posterior to the byssal sinus, the other below the umbo, leaving posterior 
 to it the greater portion of a shallow triangular depression; that of the right valve is 
 similar, with folds corresponding to the depressions of the former. Adductor 
 impression very large. Surface with a very large number of close radiating coste, 
 crossed by equally numerous concentric lamine, the cost on the right valve becoming 
 almost subordinate to the lamine. 
 
 Obs. I have not seen anything approaching a perfect specimen of the left or 
 convex valve of this species, although an impression and an excellent right valve exists 
 in Mr. Sweet’s Collection. It is the largest MWaccoyella—a mutilated left valve obtained 
 by Prof. Tate at Lake Eyre, in South Australia, measuring four inches from anterior to 
 posterior, and four and a-half inches from the dorsal to the ventral margin. Mr. Sweet’s 
 right valve is six inches in transverse measurement, and five and a-half inches in the 
 contrary direction. I think there is little doubt also that our Pl. 23, fig. 4, is this 
 species, and represents an exfoliated right valve, with the umbo and crenulations of the 
 left anterior dorsal margin perceptible above it. The impression of the left valve 
 referred to above measures five inchesin both directions. The radiating coste are very 
 numerous, and appear to extend beyond the ventral margin as spinous prolongations, 
 sunilar to MW. Barklyi, var. marieburiensis (Pl. 42, fig. 4). The coste are crossed by 
 moderately wide growth-laminw, which, at the points of intersection, project as half- 
 spines or frills. 
 
 The structure of the hinge in J. umbonalis is remarkably interesting, differing 
 in some degree from that of JZ. reflecta, and paving the way for the structure of that 
 of WW. corbiensis. 
 
 The large shell from Maryborough (PI. 23, fig. 4), apparently either much 
 decorticated, or split in half, with the shelly layers remaining along the hinge-line, 
 measures five inches by four and a-quarter, and there are still remaining indistinct 
 traces of the radiating coste. An imperfect specimen in the Mining and Geological 
 Museum measures six inches transversely from side to side, and four from the left 
 umbo to the imperfect front or ventral edge. Another, still less perfect, from the 
 Australian Museum Collection, is four and a-halfinches by four. These measurements 
 will show that IL. reflectu attained a large size. 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke) ; Bungeworgorai Creek, near 
 Mount Abundance (G. Sweet—Colln. Sweet, Melbourne). Occurs also in the Mary- 
 borough Beds—Desert Sandstone. 
 
 MaccoyeLua corBIENSIS, Moore, sp., Pl. 22, figs. 8 and 9. 
 
 Avicula corbiensis, Moore, Quart. Journ. Geol. Soc., 1870, xxxi., p. 246, t. 11, f. 7. 
 Crenatula ? gibbosa, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 339, t. 19, f. 3. 
 
 Sp. Char. Shell longitudinally ovate, longer than wide, somewhat deltoid, 
 nearly equilateral. Left valve very convex, longitudinally curved, area about 
 one-third the width of the shell, much arched, with numerous fine ligamental 
 
459 
 
 furrows; umbonal fold very excentric and oblique ; byssal fold obsolete; byssal 
 sinus probably narrow and long; anterior end rounded, with the foldings of its dorsal 
 margin numerous but not strongly marked; no wing, or ear; posterior end rather 
 produced ventrally, semi-trunecate, with a short incomplete wing (when perfect) ; ventral 
 margin broadly rounded; umbo elevated, deep, much incurved, and acute, its cavity 
 hollow ; adductor impression very excentric, concentrically ridged; pallial impression 
 marked by a series of vertically impressed fibre scars; surface with a large number of 
 radiating and bifurcating cost; the intercostal spaces, or valleys, crossed by fine con- 
 centric lines of growth, convex.in the direction of the dorsal margin. 
 
 Obs. By a series of specimens with the shell preserved, and another of internal 
 casts in the Collections of Messrs. T. W. E. David and G. Sweet, I have satisfied myself 
 that the peculiar cast described by Mr. R. Etheridge, F.R.S., as Crenatula ? gibbosa is that 
 of the left valve of this species. Imperfect examples only are now figured (PI. 22, figs. 
 8 and 9), but in a supplementary work on Queensland Paleontology, a complete set of 
 illustrations will be given. The right valve is not known with certainty. 
 
 In the outward form of the left valve this species resembles a Gryphaa, especially 
 in the overhanging sharp umbo. It also presents some features like those of Hinnites, 
 and some Oysters with hollow umbonal cavities. The peculiarities of the hinge structure 
 are best seen in the internal casts, such as figured by Mr. Etheridge, under the name 
 of Crenatula? gibbosa, and in which the infilling of the hollow umbonal cavity is always 
 well displayed. In fact, the short, almost triangular area seems to form a kind of shelf 
 across the cavity of the valve similar to that in some proboscidiform rostrate oysters. 
 
 The dorsal margin of this species is in the left valve much arched, widening out 
 below the umbo into a more or less concave somewhat triangular cartilage area, excen- 
 trically divided by the umbonal fold as an oblique prominent ridge, the ‘anterior half 
 of the area being thus much the smaller. The byssal fold is practically obsolete, and 
 the anterior :crenulations of the dorsal margin but little developed. In casts the 
 triangular outline of the area is more pronounced, and the umbonal fold is represented 
 by an oblique groove. 
 
 To some extent the typical Maccoyella hinge structure is not at first apparent in 
 this shell, but its generic affinity becomes apparent when viewed in connection with 
 that of IZ. wmbonalis. 
 
 The adductor impression is always large, and well to the posterior side. 
 
 It is possible that the impression of a very convex valve (Pl. 22, fig. 9) from 
 Maryborough may be referable here. It possesses eighteen chief ribs, with smaller 
 intermediate ones, straight, regular, and apparently non-spinous. The concentric 
 lamine are strongly marked, and the finer and more delicate parallel wrinklings equally 
 apparent. 
 
 Loc. Mount Corby (Lhe late Rev. W. B. Clarke); Bungeworgorai Creek, near 
 Mount Abundance (G. Sweet—Colln. Sweet, Melbourne); Blythe’s Creek, near Blythes- 
 dale Station (@. Sweet—Colln. Sweet, Melbourne) ; Lake Eyre, South Australia (Prof. 
 EF. Tate—Colln. Adelaide University). 
 
 Maccoverta? susstriata, Moore, sp., Pl. 22, fig. 10, ? Pl. 23, figs. 8 and 9. 
 Avicula substriata, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 247, t. 11, f. 6. 
 
 Sp. Char. Shell of medium size. Left valve very convex or subangular in 
 the middle line longitudinally ; posteriorly very alate and extended; dorsal margin, 
 or hinge-line, very long on the posterior side, but on the anterior oblique from the 
 umbo forwards, and much thickened, folded, and crumpled, forming a wide byssal 
 sinus; posterior end very wide, alate, and extended; umbo prominent, and probably 
 
460 
 incurved ; anterior and ventral margins rounded; surface bearing radiating costae, 
 which become stronger on the posterior wing, each pair separated by a smaller inter- 
 polated rib, the whole crossed by wavy, delicate, laminar frills, least conspicuous on the 
 posterior wing. 
 
 Obs. The present shell is believed to be Moore’s species (although he describes 
 it as small) from the great expansion of the posterior wing, the absence of an anterior one, 
 and the general. resemblance to his figure. If not Moore’s species, it must be an 
 undescribed form. The folded and crumpled anterior dorsal margin is a typical feature 
 of a Maccoyella, and we thus have a very interesting morphological change from the 
 shorter posterior wing of IZ. Barklyi to the lengthened condition of that portion of the 
 shell in the present species. The subangular convexity of the umbonal region is also a 
 marked feature ; and should this form prove distinct from IL. substriata, Moore, it may 
 be called WZ. subangularis. The above characters have been chiefly derived from a 
 specimen in Mr. Sweet’s Collection. 
 
 Loc. Bungeworgorai Creek, near Mount Abundance (G. Sweet—Colln. Sweet, 
 Melbourne) ; Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Genus—A UCELLA, Keyserling, 1846. 
 (Reise in das Petschora-Land, p. 297.) 
 
 Gen. Char. “ Obliquely elongated, inequivalve, of thin structure, pearly within, 
 and with concentric suleations externally; left valve strongly convex, with incurved 
 beaks, a short posterior and an almost obsolete anterior ear, represented by a slight internal 
 thickening ; margin of shell in front below the beak insinuated; right valve flat or 
 slightly convex near the umbo, with a small indistinct posterior and a still shorter 
 anterior ear, generally a little twisted, and separated from the margin below by a deep 
 byssal sinus ; hinge-line in both valves straight, short, and in the right valve usually 
 with a small blunt tooth, ligament external, linear; muscular scars small, posterior, 
 submarginal, anterior placed near the ear, and often almost obsolete.” (Stoliczka.) * 
 
 Obs. Dr. Stoliczka’s description of this interesting genus is quoted, as being the 
 best and most comprehensive with which I am acquainted; it is to all intents and 
 purposes the same as the original by Von Keyserling. 
 
 By most authors Awcella is said to be a Jurassic genus, but Eichwald believes the 
 rocks from which the original examples were procured by Keyserling to be of Cretaceous 
 age. Species definitely known to be of this period have been described by Stoliczka, 
 Gabb, Conrad, and others, and there now appears to be no doubt of its existence during 
 the epoch in question. 
 
 AUCELLA HUGHENDENENSIS, Etheridge, sp., Pl. 25, figs. 1-6. 
 
 Avicula hughendenensis, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 346, t. 25, f. 3. 
 Aucella Liversidgei, Etheridge fil., Journ. R. Soc. N. 8. Wales, for 1883 [1884], xvii., p. 90, 2nd plate (top 
 and lower right-hand figs.) ; 
 
 Sp. Char. Obliquely sub-deltoid, very inequivalve, plano-convex. Left valve 
 convex, inoceramiform, gibbous, and narrowed about the umbo, expanding ventrally , 
 beak or umbo prominent and much-incurved anteriorly, greatly overhanging the hinge- 
 line; anterior side vertical, the margin almost straight, and when seen from the inside 
 deeply insinuated under the beak ; posterior side steep, obliquely expanding ; posterior 
 ear and hinge margin very short ; ventral margin obliquely rounded ; surface with faint 
 concentric undulations, which become more apparent and laminar towards the ventral 
 margin. Right valve gently convex or prominent about the umbonal region, flattened 
 
 *Pal. Indica (Cret. Fauna), 1871, iii., fasc. 5-8, p. 390. 
 
 
 
 
 
 
 
 ee 
 
 eee is 
 
 ani i 
 
 OO —— = SO 
 
461 
 
 towards the ventral portion, obliquely rounded, with a larger and better developed 
 posterior ear than in the left valve ; anterior margin rounded ; anterior ear more or less 
 triangular, reposing completely in the insinuation of the anterior margin of the left 
 valve, separated from the body of its own valve by a deep byssal sinus; beak small, but 
 sharp and prominent. Hinge-line of both valves short, but longest in the right; no 
 tooth visible in the interior of the right valve. Both valves are crossed by fine radiating 
 strize which give rise to a minute cancellation; in the left valve the strie are more 
 apparent below the beak, and die out on the body of the shell; in the right valve they 
 are of a fluctuating or wavy character, and the concentric lamine become frill-like ; 
 surface highly polished. 
 
 Aucella hughendenensis is undoubtedly allied to two types of the genus, 
 A, Pallasii, Keyserling,* and A. crassicollis, Keys.t In possessing the obliquity and 
 short hinge-line, it resembles the former; the left valve has the general form of the 
 latter species and a similar much incurved beak, whilst the right valve in all its 
 peculiarities is almost identical with that of A. Pallasii. The resemblance of our shell 
 to and its intermediate position between the two species in question is very remark- 
 able. A. hughendenensis is also allied to the Indian Cretaceous species A. parva, 
 Stoliczka,t but the left valve in the former is more inoceramiform than in the latter, 
 and more oblique. 
 
 In A. speluncaria, Schlotheim,§ there are radiating striz, but our species is less 
 deltoid and more regular, and there is no inflection of the ventral margin. 
 
 A. Hausmanni, Goldfuss,|| from the Zechstein of Scharzfeld, is a much more 
 slender shell than the Australian species, less convex, and more elongate from the beaks 
 to the ventral margin. Another species, A. cawcasica, Abich,¥ possesses fine radiating 
 strie, to say nothing of the larger ear in the right valve, a more pointed and prominent 
 umbo in the left, and a generally different outline to the valves. There appears to be 
 at least one very interesting British example of Aucella, the A. grypheoides, J. de C. 
 Sowerby, sp.,***but it hasa much larger umbo in the left valve, and the general characters 
 of the right are quite different. 
 
 The last species with which I am able to compare A. hughendenensis is the 
 American Cretaceous form of A. Piochii, Gabb,t+ avery gibbous and thick shell through 
 the valves, quite distinct from the Australian. It is not related to A. plicata, Zittel,tt 
 which differs in form, and has coarse concentric corrugations over the valves. 
 
 Aucella hughendenensis was no doubt a very abundant species, and probably 
 gregarious, ‘“‘masses of them occurring together, forming a ccmpact and dense 
 argillaceous limestone.”§§ It was equally variable, for in some the radiating strize only 
 predominate ; in others a reticulation caused by the presence of transverse concentric 
 lines is the main feature. ‘T'wo or three of the radiating ribs sometimes become very 
 much larger and prominent. The smaller valve has at times an almost Anomia-like 
 appearance, sometimes a little gnarled, and corrugated by three or four concentrie 
 ridges and corresponding depressions. In individuals of more advanced age the 
 
 
 
 
 
 * Reise in das Petschora-Land, p. 299, t. 16, f. 1-7. 
 
 + Ibid., p. 300, t. 16, f. 9 and 12. 
 
 + Pal. Indica (Cret. Fauna), 1871, iii., fas. 5-8, p. 404, t. 33, f. 2 and 3. 
 
 § See Geinitz, Dyas, t. 14, f, 5-6. 
 
 || Mytilus, Petrefacta Germania, ii., p. 168, t. 138, f. 4; Awcella, Geinitz, Dyas., p. 72, t. 14, f. 85. 
 
 { Zeitsch. deutschen Geol. Gesellsch., 1851, iii., p. 31, t. 2, f. 1. 
 
 ** Trans. Geol. Suc., iv., t. ii., f. 3. 
 
 ++ Pal. California, ii., t. 32, f. 92. 
 
 +t Reise Oesterr. Fregatte ‘‘ Novarra,” 1857-59, Geol. Theil, Band I., 2 Abth., 1865, p. 32, t. 8, f. 4a-c. 
 §§ Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 346, 
 
462 
 
 radiating strize became almost ribs, and the concentric lines nearly died out. Locality 
 appears to have had an influence on the size of the shell; thus, those at Aramac are 
 rather small, those at the Barcoo larger. 
 
 The inner layers of shell have a silky lustre, with very fine anastomosing, 
 concentric lines. A very thin and delicate shell occurs at Blackall Well, which has 
 all the surface characters of this species, except that the concentric lines are finer or 
 more prominent. It may, perhaps, be a distinct species. 
 
 Loc. Wughenden Station, Flinders River (The late R. Daintree ; The Hon. A. C. 
 Gregory); Rockwood Station, Landsborough. River, in a light-drab shelly limestone 
 (Prof. A. Liversidge—Colln. Sydney University; &. ZL. Jack); Flinders River, seven 
 miles above Marathon Station, in a dark-drab limestone (R. LZ. Jack); Marathon 
 (G. Sweet—Colln. Sweet, Melbourne) ; Neelia Creek, at crossing of the Cloncurry Road, 
 in a light-drab limestone (#. L. Jack); Aramac Well, at a depth of two hundred and 
 forty-four feet (S. Sharwood); Coorena Woolshed, twenty-four miles south of Aramac 
 (Rk. L. Jack) ; Stone Hat, Rockwood Creek, Landsborough River, in a drab shelly lime- 
 stone ; Landsborough River, five and a-half miles north-north-west of Rockwood Station, 
 in a yellow-drab arenaceous limestone; Jirking Creek, near its head, in a greenish 
 limestone; Leichhardt River, seven miles from mouth of Gunpowder Creek, in a dense 
 cream-coloured limestone (2. L. Jack) ; Warrianna Bore, at three hundred and fifty-one 
 feet (J. B. Henderson); Barcoo River, right bank, six miles above Northampton Downs 
 Station (R. L. Jack). 
 
 Genus—PERNA, Brugquiére, 1789. 
 (Tab. Encyclop. Method., Pl. 175.) 
 
 PERNA GIGANTEA, Moore. 
 
 Perna gigantea, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 249. 
 Sp. Char. Shell very large, measuring six and a quarter inches broad by five and a 
 half inches in length, flattened ; umbones depressed and rather produced ; anterior byssal 
 area rounded ; hinge-line rather oblique, extending one-third the width of the shell; 
 
 posterior end oblique, rounded, and folding towards the ventral margin, which, with the © 
 
 anterior end, is rounded. (Joore.) 
 Obs. P. gigantea was associated with Lingula ovalis, and a Mytilus, both 
 species characteristic of the Wollumbilla blocks. The shell has not been figured, nor 
 has it occurred to me in any of the Collections examined. 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 Genus—INOCERAMUS (J. Sowerby, 1814, m.s.), Parkinson, 1819. 
 (Trans. Geol. Soc., v., p. 55.) 
 
 Obs. The genus Inoceramus was proposed and described in a Paper read before 
 the Linnean Society of London on 1st November, 1814, by the late Mr. James Sowerby, 
 entitled ‘On a Fossil Sheli of Fibrous Structure,” &c. The description was published 
 in December, 1822 ;* but, in the meantime, between the dates of reading and publication 
 of Sowerby’s paper, Parkinson published a description—viz., in 1819 +—which must, 
 therefore, be accepted as the real date of the publication of Inoceramus, and not 1814, 
 as is usually given in works. 
 
 
 
 * Trans. Linn. Soc., xiii., Pt. 2. 
 + Trans. Geol. Soc., v., p. 55. 
 
 ———— a 
 
4.63 
 
 The Queensland Znocerami appear to indicate an borizon near that of the Lower 
 Chalk, although in a collection of fossils forwarded to England by Mr. W. Hann, from the 
 Bareoo River, fifty miles below its junction with the Alice River, Mr. R. Etheridge, 
 F.R.S., recognised species having the general facies of British Gault forms. * 
 
 The great variability of the shells forming the genus Inoceramus renders it very 
 difficult to decide on the specific identity of its individuals, and the succeeding 
 determinations can only be accepted as provisional. As regards the Australian 
 species, this is increased by the fact that in the majority of cases the specimens are 
 either too ill-preserved, or too fragmentary, to yield satisfactory results. Specimens of 
 a drab-coloured limestone have been collected by my Colleague on the Flinders River, 
 seven miles above Marathon Station, and a calcareous flaggy bed the same distance 
 below the Station, entirely composed of the remains of Jnocerami. On the Cloncurry 
 Road, in localities eight and fifteen miles west of Williams River, a white porous rock 
 is completely built up of the disintegrated shelly matter of this genus; whilst at the 
 second of the localities just mentioned specimens of an argillaceous limestone have 
 been obtained, with the weathered surfaces covered with white spicular or needle- 
 shaped bodies, which are nothing more than the broken-up prisms of the prismatic 
 shell-structure of ZInoceramus. These instances will serve to show the relatively great 
 abundance of Inoceramus in the North Queensland Cretaceous Series. 
 
 Inocrramus Carsont, McCoy, Pl. 25, figs. 9 and 10. 
 Inoceramus Carsoni, McCoy, Ann. and Mag. Nat. Hist., 1865, xvi., p. 334; Ibid., 1867, xx., p. 196. 
 
 PY) 3 McCoy, Trans. R. Soc. Vict., 1866, vii., p. 50. 
 5 allied to I. problematicus (D’Orb.), Etheridge, Quart. Journ, Geol. Soc., 1872, xxviii., p. 344, 
 taco. tors 
 
 Obs. Both Prof. Sir F. McCoy and Mr. R. Etheridge, F.R.S., call attention 
 to the resemblance of their respective shells to Incceramus mytiloides, Sby.; and the 
 characters mentioned by the former appear hardly sufficient to separate the species. 
 Prof. McCoy states that his shell differs from the British “in having the hinge-line 
 rather longer, the anterior end more pointed, and the superior posterior angle rather 
 more obtuse.’’ The undoubted resemblance borne by Mr. Etheridge’s fig. 4, Pl. 22, to 
 the general figures of Inoceramus problematicus, D’Orb. (I. mytiloides, Mantell and 
 Sby.), renders it necessary to unite it with McCoy’s LZ. Carsoni. No absolute description 
 of the Australian shell has yet ever appeared, comparison thereby becoming difficult. 
 
 The elongated, somewhat narrow form appears to be the chief character of the 
 species. The shell of those examples I have referred to it is nearly a quarter of an inch 
 thick, and the structure very coarsely fibrous. 
 
 Loc. Base of Walker’s Table Mountain, Flinders River (Messrs. Carson and 
 - Sutherland—National Museum, Melbourne) ; Marathon Station, Flinders River (The 
 late R. Daintree) ; ? Landsborough Creek, Thomson River (Prof. A. Liversidge—Colln. 
 Sydney University) ; Flinders River, three miles above Richmond Downs Station, in 
 drab limestone ; and thirteen and a-half miles below the same, in an argillaceous lime- 
 stone, with a cone-in-cone structure (R. L. Jack). 
 
 InoceramMus SutuerRLAnndtI, McCoy. 
 
 Inoceramus Sutherlandi, McCoy, Ann. and Mag. Nat. Hist., 1865, xvi., p. 884; Ibid., 1867, xx., p. 196. 
 Bs ap McOoy, Trans. R. Soc. Vict., 1866, vii., p. 50. 
 
 Obs. Prof. Sir F. McCoy refers to this shell as much larger and broader than 
 L. Carsoni. “In form, size, and concentric undulations of the surface nearly agrees 
 with the French and English common Cretaceous 7. Cuviert, but is less curved at the 
 
 
 
 
 
 * Quart. Journ. Geol. Soc., 1872, xxviii., p. 183. 
 
464. 
 
 ventral margin near the beak, and rather narrower and more acute at the anterior end.” 
 I. Cuvieri is such a distinctive and well-marked shell that it is better to retain the 
 present species separate. 
 
 Lor. Base of Walker’s Table Mountain, Flinders River (Messrs. Carson and 
 Sutherland—National Museum, Melbourne); Flinders River, three miles above 
 Richmond Downs Station, in drab limestone; and twenty-one miles below the Station, 
 in a similar rock (R. L. Jack). 
 
 INOCERAMUS PERNOIDES, Etheridge, Pl. 25, figs. 7, 8, and 12. 
 Inoceramus pernoides, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 3438, t. 22, f. 3. 
 
 Sp. Char. Shell quadrate, deep; umbonal region thick and elevated; beaks 
 acute; anterior side slightly convex; the ventral margin broadly rounded; surface 
 marked by alternating groups of fine and coarse concentric folds, or large undulations. 
 (Htheridge.) 
 
 Obs. This shell much resembles J. regularis, D’Orb., in shape, size, and mark- 
 ings, but the wing or hinge-area is not so long. It is almost identical in shape with 
 I. Lamarckii, I. latus, and I. crispus, Mant., but the concentric undulations are not so 
 unequal and pronounced, neither had this shell a corrugated and thickened fold along 
 the hinge-line, as in I. Lamarckii ; the teeth or hinge-pits are not seen. Itis evident that 
 this is an abundant species in the Cretaceous rocks of Queensland, its remains being 
 numerous and usually fragmentary. (£theridge.) 
 
 A large shell (Pl. 42, f.7) measuring six inches in length and four wide, the 
 longest diameter being still incomplete, may perhaps be referred here. In its present 
 state it is an internal cast, and is but indifferently figured. 
 
 Loe. Marathon Station, Flinders River (The late R. Daintree) ; Flinders River, 
 seven miles above the same, in dark-drab limestone (R. L. Jack) ; Well, at two hundred 
 feet below surface, seven miles east of Mount Cornish Homestead (#. Hdkins). 
 
 INOCERAMUS MARATHONENSIS, Htheridge. 
 
 Inoceramus marathonensis, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 348, t. 22, f. 1. 
 “ Etheridge fil., Journ. R. Soc. N, S. Wales, 1883, xvii., 1st pl., up. fig. 
 
 Sp. Char. Shell elongated and compressed ; umbonal region narrow, acute, and 
 tapering; ventral portion of shell much expanded; concentric plications or undulations 
 variable, being alternately broad and narrow, and unequal. (theridge.) 
 
 Obs. In size and shape it somewhat resembles 7. annulatus from the White 
 Chalk of Westphalia ; but the want of the true outer shell prevents our referring it to 
 that species, the equidistant lines of growth in J. annulatus being characteristic and 
 well defined. (theridge.) 
 
 This is retained provisionally asa species. The elongated form, and very coarse’ 
 corrugations, with intermediate fine concentric lines appear to distinguish it. If 
 Inoceramus Sutherlandi, McCoy, is after the type of Z. Ouvieri, the present shell is a 
 separate and distinct species, so far as Australian Inocerami are concerned. 
 
 Loc. Marathon Station, Flinders River (The late R. Daintree); Landsborough 
 Creek, Thomson River (Prof. A. Liversidge—Colln. Sydney University). 
 
 INOCERAMUS ELONGATUS, Htheridge. 
 
 Inoceramus multiplicatus, Stoliczka, var. Hatha Etheridge, Quart. Journ. Geol. Seas 1872, xxviii., 
 p. 343 (excl. ref.), t. 22, £.°2. 
 
 Sp. Char, Shell much elongated, ok numerous concentric ribs, which become 
 coarser and flatter near the ventral margin; umbones acute and apparently incurved ; 
 whether they approximate or not, we have no means of determining. (theridge.) 
 
465 
 
 Obs, The following remarks were madé by Mr, Etheridge :—With the exception 
 of being more elongated than the shell described by Dr. F. Stoliczka, our shell appears 
 to be the same, allowing for those variations which the species in this genus exhibit. It 
 is not so ventricose a shellas L. striatus, Mant., from the Lower Chalk of Sussex, Saxony, 
 &e. (Etheridge.) 
 
 I fail to detect any direct resemblance between the figure of this bivalve and that 
 of Stoliczka’s JZ. multiplicatus.* It will possibly simplify matters if it be known under 
 its varietal name, elevated to specific rank, until more definite characters can be assigned 
 to it than those quoted above. 
 
 The peculiarity of the concentric folds removes it from J. problematicus (D’Orb.) ; 
 and as regards I. multiplicatus, it differs wholly in shape. 
 
 Loc. Marathon Station, Flinders River (The late R. Daintree). 
 
 Inoceramus Cripstr, Mantell, ? Pl. 21, figs. 17 and 18. 
 Inoceramus Cripsti, Mantell, Foss. 8. Downs, 1822, p. 183, t. 27, f. 11. 
 
 ed 99 Zittel, Denks. K. Akad. Wissensch. Wien, 1866, xxv, Abth 2, p. 95, t. 14, f. 1-5, t. 15, 
 f. 1-5. 
 
 ‘e 3 F. Roemer, Kreidebild. Texas, 1852, p. 56, t. 7, f. 2. 
 
 » Cripsianus, Stoliczka, Pal. Indica (Cret. Fauna), 1871, iii., fas. 5-8, p. 405, t. 27, f. 1-3. 
 
 Obs. Several examples of an obliquely-oval oblong Inoceramus have been 
 collected by Mr. 8S. Sharwood at Aramac Well, with coarse, distant, regular, and even 
 corrugations, which I cannot with any degree of accuracy separate from this world-wide 
 species, known as it is from Europe, India, and America (Texas). 
 
 The individuals are constant in size and shape, possessing a stronger resemblance 
 to Prof. Zittel’s excellent figures than they do to Stoliczka’s of the Indian variety. We 
 observe the straight hinges, oblique-oval form, prominent anterior, and almost terminal 
 beaks, and the same angular, concentric, sometimes fluctuating corrugations, with inter- 
 mediate finer strie. The only difference which can be detected is the smaller and deeper 
 anterior end, but, as I have not succeeded in entirely relieving a specimen from the matrix, 
 the latter, and verified examples of I. Cripsi?, cannot be compared in this direction. 
 
 There also exists a resemblance to Inoceramus proximus, Meek,t more especially 
 in the smaller anterior end; and a further comparison may be made with Jnoceramus 
 problematicus, var. aviculoides, Meek.t 
 
 A small form of Znoceramus has been met with in a boring at Muttaburra. The 
 outer shell has been removed, and the outline is not entire, but there are still traces of 
 the usual corrugations. This may be the decorticated condition of Inoceramus Cripsii. 
 It is certainly after that type. 
 
 Loe. Aramac Well, at depths of two hundred and thirty-eight feet and two 
 hundred and forty-four feet, respectively GS. Sharwood); Muttaburra Bore (J. B. 
 Henderson). 
 
 Family—PINNIDZ. 
 Genus—PINNA, Linneus, 1758. 
 (Syst. Nat., Ed. x.) 
 Pinna, sp. ind., P|. 20, figs. 16 and 17. 
 
 Obs. Amongst the Walsh River fossils is the posterior end of a large Pinna, 
 four and a-half inches long, with a width of three and a-quarter inches. The shell is 
 
 
 
 * Pal. Indica (Cret. Fauna), 1871, iii., fas. 5-8, p. 406, t. 28, f. 1. 
 + Report U.S. Geol. Survey Ter., 1876, ix. (Invert Cret. Tert, Foss, Up. Missouri), p. 53, t. 12, f. 7a, 
 ft Loca cit., p. 63, t..9, £4 
 
 2F 
 
4.66 
 
 more or less preserved, and bears indistinct, obtuse, longitudinal ribs, crossed by very fine 
 imbricating lamelle of growth. It is closely allied to Pinna laticostata, Stoliczka,* 
 from the Arrialoor Cte of India, and may possibly be so to Pinna australis, 
 Hudleston.+ 
 
 Loc. Walsh River (Hon. A. C. Gregory). 
 
 Family—MYTILIDZ. 
 
 Genus—MYTILUS (Linneus), Lamarck, emend., 1799. 
 (Prodrome—Mém. Soc. Hist. Nat. Paris, 1799, p. 88.) 
 
 Mytitus TENISONWOODST, sp. 200. 
 Mytilus planus, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., Pt. i., p. 252, t. 18, f. 3. 
 
 Sp. Chay. Shell small, thin, ovate, compressed, nearly equilateral; umbones 
 terminal and acute, ventral margin rounded; dorsal surface smooth, with depressed 
 concentric lines of growth, Sale by very ae radiating lines, which wholly cover the 
 exterior. Its flattened form, with its distinct ornamentation, readily distinguishes the 
 species. (JZoore.) 
 
 Obs. The specific name applied by Mr. Moore to this shell had already been — 
 twice used before in the same sense. Eichwald employed it in the first instance for 
 a supposed Paleozoic Mytilus, but afterwards referred the shell to Avicula.t Kloden 
 has likewise used the name planus for a Mesozoic Mytilus,§ and under these circum- 
 stances less confusion will be caused by changing it than by retaining it for the 
 above shell. The name of the late Rev. J. E. Tenison Woods may appropriately 
 be associated with it, as a very slight recognition of his labours in Queensland 
 Paleontology. 
 
 As the interior of this shell-is entirely covered with radiating lines, it may 
 perhaps be referable to the genus Crenella, rather than to Mytilus proper. 
 
 Loe. Wollumbilla (The late Rev. W. B. Clarke). 
 
 Mytiuvus rvuaocostatus, Moore. 
 Mytilus rugocostatus, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 252, t. 13, f. 2. 
 
 Sp. Char. Shell thick, ovately oblong ; umbones terminal and acute; posterior 
 margin oblique and curved ; anterior side prodaced and somewhat rounded; the dorsal 
 surface is obtusely Peeled? and towards the umbo has very coarse irregular concentric 
 striz or lines of growth, which become finer towards the ventral margin. (dZoore.) 
 
 Obs. Unlike the Mytilide generally, whose shells are usually thin and fragile, 
 this species possesses a very thick test, especially in adult examples. When a 
 portion of the test has adhered to the matrix, leaving an inner layer exposed on the 
 shell, the strie are not seen, and the surface appears smooth, giving it the appearance 
 of an entirely different species. (JZoore.) 
 
 Mr. G. Sweet has found at Bungeworgorat Creek, a Mytilus, two and a-half 
 inches long, which is probably this species. 
 
 I suspect that the Mytilus, sp.,|| recently figured by Mr. Hudleston from the 
 Lake Eyre Basin is but a well preserved cast of the present species. 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke) ; Bungeworgorai Creek (G. 
 Sweet—Colln. Sweet, Melbourne). 
 
 
 
 
 
 * Pal Indica (Cret. Fauna), 1871, iii., p. 385, t. 25, f. 2 and 3. 
 + Geol. Mag., 1890, vii. (3), p. 244, t. 9, f. 6. 
 
 + Letheea Rossica, ii., p. 946. 
 
 § Verstein, Mark Brandenburg, 1834, p. 207, Gr Ostend 
 
 || Geol. Mag., 1890, vii. (3), p. 245, t. 9, f. 9, 
 
467 
 
 Myrinvs wnFiatus, Moore, Pl. 25, fig. 11. 
 
 Mytilus inflatus, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 252, t. 13, f. 4. 
 5p 45 Ten. Woods, Journ. R. Soc. N. g, Wales, 1882 [1883], xvi., p. 153, t. 10, f. 8. 
 
 Sp. Char. Shell smooth, slightly inequivalve, convex, both valves inflated ; 
 margins close-set ; umbones terminal, acute, anterior; hinge-line extended and oblique ; 
 posterior margin and front rounded ; dorsal surface smooth, with irregular concentric 
 bands of growth. (JMoore.) 
 
 Obs. ‘This pretty little shell is to be distinguished by its very inflated appear- 
 ance, its more extended hinge-line, and terminal umbones. Its test still retains some 
 Rels. ” ( Moore.) 
 
 The specific name of this species was preoccupied by Miiller before it was made 
 use of by Mr. Moore, but the species described by the former is referable to another 
 pre-existing species,* wherefore the name ascribed by Mr. Moore to the Australian shell 
 will probably stand. 
 
 The late Rev. J. E. T. Woods believed WZ inflatus to be of Oolitic age. There 
 is, however, no absolute reason for considering it as so differing from the other fossils 
 with which it is associated. 
 
 -Althouwh represented as a longer shell, I think that Mr. Hudleston’s Modiola 
 linguloides + is only a variety of the present species, and I notice that Prof. R, Tate 
 places it as a synonym,t and more recently still this is admitted by Mr. Hudleston.§ It 
 is very abundaut in the Lake Eyre Beds, and I had an opportunity of examining a large 
 series forwarded to the Indian and Colonial Exhibition by Mr. H. Y. L. Brown. Mr. 
 Tenison Woods’ figure represents a still larger individual, and one posteriorly so much 
 more lengthened than Moore’s figure, that I would prefer for the present to withhold a 
 conclusive opinion as to its identity. Between the bands of growth the shell is covered 
 with very delicate concentric strie. I was indebted to the late Mr. Tenison Woods for 
 the loan of his figured specimen. 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke); Palmer River (The late Rev. 
 J. H. T. Woods). 
 
 Myritus 1ncEns, Ten. Woods. 
 Mytilus ingens, Ten. Woods, Proc, Linn, Soc. N.S. Wales, 1882, vii., Pt. 3, p. 389. 
 
 Sp. Char. Shell oblong, oval or elliptical, tumid, or gibbous in the centre, so as 
 to form an arched, broad, regularly sloping carina, depressed at the anterior side; 
 thick, but not clumsy, at the posterior margin ; the whole very equally sulcate with lines 
 _of growth, the younger*ones deep-ridged and with a beautiful curve, the latter less 
 distinct. Umbones terminal, small, corroded, curved. Ligamental fossa somewhat small, 
 broad, terminal, shallow, with a long, narrow slit for the byssus. Pallial impression 
 long and wedge-shaped. Length thirty centimetres, breadth nineteen, height seventeen, 
 length of hinge depression nine. (Zen. Woods.) 
 
 Obs. This appears to be a very large species, and distinct from either of those 
 described by the late Mr. C. Moore from the Wollumbilla blocks, although in form it 
 approaches I. inflatus, Moore. 
 
 Loc. Barcoo District (Lhe late Rev. J. H. T. Woods). 
 
 * See Stoliczka, Pal. Indica (Cret. Fauna), 1871, iii., fase. 5-8, p. 373. 
 + Geol. Mag., 1884, i., p. 341, t. 11, f. 6 a-b. 
 
 t+ Proc. Austr. Assoc. Adv. Sci. for 1888 [1889], i., p. 280, 
 
 § Geol. Mag., 1890, vii. (3), p, 245, 
 
468 
 
 Genus—MODIOLA, Lamarck, 1799. 
 (Prodrome—-Mém. Soc. Hist. Nat. Paris, 1799, p. 87.) 
 Moprota wntca, Moore. 
 Modiola unica, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 253, t. 18, f. 5. 
 
 Sp. Ohar. Shell small, smooth, obtuse, convex, thickest at the umbones ; 
 umbones subterminal; hinge-line straight ; anterior side produced and rounded ; 
 dorsal surface, with a few flattened concentric striw, which are decussated by very 
 faint longitudinal lines. (oore.) 
 
 Obs. This shell has much the appearance of a Lithodomus. 
 
 Loe. Wollumbilla (The late Rev. W. B. Clarke). 
 
 Order—UNIONACEX. 
 Family—UNIONIDZ. 
 
 Genus—UNIO, Phillipsson, 1788. 
 (Dissert. His. Nat. Nov. Test. Genera, p. 26.) 
 Obs. Two specimens of Unio were obtained from the sinking of the Government 
 Well at Winton. The specimens seem to be distinct from one anothergand are both 
 small forms. They were presented to the Geological Survey Museum by Mr. Julius 
 von Berger, 
 
 Order—ARCACEA. 
 Family—ARCID. 
 
 Genus—ARCA, Linneus, 1758. 
 (Syst. Nat., Ed. x., i., p. 693.) 
 
 Arca PRELONGA, Moore, Pl. 33, fig. 7. 
 Arca prelonga, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 249, t. 14, f. 7. 
 
 Sp. Char. Shell transverse, inequilateral; umbones rather close, anterior ; 
 hinge-line long, with numerous close-set teeth; posterior side extended and slightly 
 angulated, with a depressed keel crossing from the umbo to the posterior ventral margin. 
 (Moore.) 
 
 Obs. Had it not been for the mention of “close-set teeth,’ I should have 
 considered the reference of this shell to Arca very doubtful. 
 
 Loe. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Genus—CUCULLA, Lamarck, 1801. 
 (Syst. Anim. sans Vertéb., p. 166.) 
 
 CucuttmA HEenpERsont, sp. nov., Pl. 26, figs. 2 and 3. 
 
 Sp. Char. Shell small, obliquely oblong, gibbous; cardinal margin straight ; 
 the area seems to have been wide, and on casts are visible the impressions of three 
 lateral teeth, a little oblique to the margin. Umbones prominent, projecting, gibbous, 
 slightly more anterior than median; anterior end moderately large, sharp-angled ; 
 posterior end rather larger than the anterior, obliquely truncated, with a well-marked 
 diagonal ridge and posterior slope, with a simple and not emarginate margin; ventral 
 margin nearly straight medianally. Surface with somewhat strong concentric lines, 
 apparently crossed by radiating striz. 
 
, 469 
 
 Obs. This is a small and neat species, and quite different from any other 
 member of this family yet described from Queensland rocks. It is named in honour of 
 Mr. J. B. Henderson, Hydraulic Engineer to the Queensland Government, who has 
 been kind enough to contribute several species for the illustration of this work. 
 
 Loc. North-east end of Glanmire Block, seventeen miles south-west of Tambo 
 (Mr. Goffage). 
 
 Family—NUCULID. 
 
 Genus—N UOULA, Lamarck, 1799. 
 (Prodrome—Mem. Soc. Hist. Nat. Paris, 1799, p. 87.) 
 
 Nvucvuna quaprata, Etheridge, Pl. 26, figs. 8 and 9. 
 Nucula quadrata, Etheridge, Quart. Journ. Geol. Soc,, 1872, xxviii., p. 341, t. 19, f. 5, t. 20, f. 3. 
 
 Obs. This species, hitherto only known from the Desert Sandstone of Mary- 
 borough, is described under the head ‘Desert Sandstone,” to which the reader is 
 referred. It has, however, been found in the Rolling Downs Formation, in the Aramac 
 Town Well, at the depth of two hundred and forty-four feet, by Mr. S. Sharwood, by 
 whom it was presented to the Geological Survey. 
 
 e Nvcura Coorrrt, Moore, Pl. 34, fig. 11. 
 Nucula Coopert, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 254, t. 12, f. 8. 
 
 Sp. Char. Shell trigonal, very convex; umbones rather anterior, widely 
 separated ; anterior side angular, posterior side rather produced and attenuated ; ventral 
 margin rounded. (Moore.) 
 
 Obs. This shell, for a Nucwla, attains considerable size. It may be distinguished 
 from Nueula quadrata, Eth., and N. gigantea, Eth., apparently by its more deltoid form. 
 
 Loe. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Nucvta truncata, Moore, Pl. 33, fig. 9. 
 Nucula truncata, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 254, t. 12, f. 9. 
 
 Sp. Char. Shell triangular ; umbones anterior, compressed; anterior side very 
 truncated; dorsal margin rounded; hinge-line with about seven large teeth on the 
 posterior side of the umbo, and with four or five on the anterior side. (JZoore.) 
 
 Obs. According to Mr. Moore, NV. truncata is readily distinguishable from 
 NV. Cooperi by its more compressed form and truncated margin. 
 
 The name must not be mistaken fora similar one used by Nilsson, for a shell 
 which is now usually referred to Nucula pectinata, Sby. I find, from South Australian 
 examples forwarded to me by Prof. R. Tate, that there is a marked posterior slope and 
 apparently a wide and long heart-shaped lunule. 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 NvcunLa AUSTRALIS, Moore, sp. 
 Leda australis, Moore, Quart. Journ, Geol. Soc., 1870, xxvi., p. 251, t. 12, f. 7. 
 
 Sp. Char. Shell transversely ovate; umbones anterior, contiguous, compressed ; 
 anterior side rounded, posterior side longest, attenuated; hinge-teeth small, numerous ; 
 dorsal surface covered with numerous transverse strize. (Zoore.) 
 
 Obs. Although described asa Leda by Mr. Moore, this shell has quite as much 
 the appearance of Nwcula, to which it is now referred. The description will apply to 
 either genus, and, like many of Moore’s species, the shell is too loosely diagnosed to be 
 easily recognisable. 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
470 
 
 Nucuta, sp. ind. 
 
 Obs. Another species, apparently differing from any of the foregoing, has been 
 obtained during the sinking of the Aramac Well. It is only known in the condition of 
 an internal cast; but this is trigonal, with a semi-pointed posterior end, a straight 
 posterior hinge, and numerous small teeth. The muscular impressions are strongly 
 marked, the anterior being situated low down, whilst a single row of dot-like sears 
 (retractor impressions?) are ranged from the yybonal cavity to the posterior adductor. 
 The margins are apparently plain. 
 
 A very similar shell to this is Nweula planimarginata, Meek,* from the Fox 
 Hills Group, of the Missouri Cretaceous. 
 
 In form this species is not unlike NV. pectinata, Sby., of the European Gault, but 
 we know nothing of the ornament as a further means of comparison. 
 
 Loc. Aramac Well, at two hundred and forty-four feet deep (S. Sharwood). 
 
 Family—TRIGONIADZ, 
 
 Genus—TRIGONTIA, Bruguiere, 1789. 
 (Encycl. Method., i., Pl. 14.) 
 
 TRIGONIA LINEATA, Moore. 
 
 Myophoria, sp., McCoy (fide Moore), Trans. R. Soc. Vict., 1865, vi., p. 44. 
 Trigonia lineata, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 255, t. 13, f. 12. 
 3 »  Lycett, Mon. Brit. Foss. Trigoniz, 1879, No. 5, p. 224. 
 
 Sp. Char. Shell thick, equivalve, inequilateral, gibbous, as broad as long ; 
 umbones convex, recurved towards the anterior margin; anterior side and ventral 
 margin rounded; posterior angle somewhat rounded; marginal ecarine absent; ‘shell 
 gradually sloping to the front; surface with close-set regular transverse concentric 
 strie, about twenty in number, which on the anterior margin possess depressed 
 tubercules. (oore.) 
 
 Obs. Mr. Moore was the first to point out that MecCoy’s Myophoria was in 
 reality a T'rigonia, and he, in accordance with this view, proposed for it the above name, 
 comparing it with the European Portlandian species, Zrigonia gibbosa. It was from the 
 supposed presence of this Myophoria that McCoy suggested the occurrence of the Rhetic 
 Formation in Australia, but it “does not possess the oblique keel and the acute 
 posterior side” of that genus. ; 
 
 It is more than likely that the late Dr. Lycett was correct when he compared 
 T. lineata with the Indian Cretaceous species 7. orientalis, Forbes,t and 7. suborbicularis, 
 Forbes,{ rather than to an Oolitic species, as suggested by.-Moore. In fact, Lycett 
 believed 7. lineata to have a strongly Cretaceous aspect. 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 TRIGONIA MESEMBRIA, Zen. Woods. 
 Trigonia mesembria, Ten. Woods, Proc. Linn. Soc. N. 8. Wales, 1883, viii., Pt. 2, p. 287, t. 12, f. 1-8. 
 
 Sp. Char. Shell ovately oblong, tumid, very convex; umbones somewhat anterior, 
 not recurved; superior border moderately convex, rather elongate; posterior border 
 curved, slightly truncate at the siphonal margin; anterior border tumidly produced and 
 rounded ; - posterior groove wide, conspicuous, shallow, widening rapidly from the 
 umbones to the margin; costz irregular, not prominent, some smaller ones occasionally 
 intercalated, all passing horizontally across the valve, slightly undulating anteriorly, 
 
 * Report U.S. Geol. Survey Ter., 1876, ix. (Invert. Cret. Tert. Foss. Up. Missouri), t. 15, f. 8a-0. 
 + Trans. Geol. Soc., 2nd Ser., vii., p. 150, t. 18, f. 11. 
 £ Lbid., p. 150, t. 18, f. 10. 
 
471. 
 
 disappearing on the posterior groove ; siphonal ridge smooth, with three narrow rounded 
 ridges, three rather wide shallow grooves between, which become faint as they widen 
 towards the margin; escutcheon long, ovate, with a flat groove on each side, strie on 
 the lower part, the rest smooth, margins raised; hinge teeth thick, large, prominent, 
 with two grooves on the upper edge, and about thirteen close, neat, parallel lateral 
 grooves; shell thick. (Zen. Woods.) 
 
 Obs. Although this shell was described from a New South Wales locality, the 
 latter is so near the Queensland border that it is thought advisable to include it here. 
 
 T. mesembria, Mr. Woods states, is one of the group Glabre, or smooth Trigonia, 
 and approaches nearest in its form to 7. dunscombensis, Lycett, from the British Upper 
 Greensand. It is said to be quite distinct from the other Australian species Z. Moore?, 
 Lycett, 7. lineata, Moore, and 7. nasuta, Eth., although in outline nearest to the latter. 
 
 Loc. Mount Stewart Run, Grey Ranges, New South Wales, near the South 
 Australian and Queensland borders (The late Rev. J. B. T. Woods-——Colln. Woods). 
 
 TRIGONIA, sp. and. (6), Pl. 21, fig 21. 
 
 Obs. A small and fragmentary but well-defined valve apparently of a Zrigonia is 
 represented in Pl. 21, fig.21. The interior is exposed, but unfortunately the umbo and 
 cardinal margin have disappeared. It possessed a ventricose appearance, a much 
 attenuated posterior end, a strongly marked diagonal ridge, and a large posterior siope 
 for the size of the valve. The latter appears to have borne three, or perhaps more, well- 
 defined ridges. The interior is highly nacreous, and when this layer is removed the 
 external impression of the shell is visible with strong concentric ridges. 
 
 This form has a strong resemblance to a small and peculiar species, 7. semiornata, 
 figured by A. D’Orbigny from the Cretaceous rocks of South America.* 
 
 Loc. Blackall Road, nine miles from Tambo, accompanied by Belemnites, in a 
 shelly limestone (2. D. Jack). 
 
 Family—ASTARTIDZ. 
 Genus—ASTARTEH, J. Sowerby, 1816. 
 (Min. Con., ii., p. 85.) 
 ASTARTE WOLLUMBILLANSIS, Moore, Pl. 27, fig. 16. 
 Astarte wollumbillensis, Moore, Quart. Journ, Geol. Soc., 1870, xxvi., p. 250, t. 12, f. 12. 
 Sp. Char. Shell small, thick, ovately orbicular, gibbous ; umbones large, mesial ; 
 posterior side rather extended, anterior slightly oblique ; ventral margin rounded ; 
 
 shell covered with numerous regular concentric rugs, with deepish interspaces, and with 
 three or four interrupted folds of growth. (JLoore.) 
 
 Obs. The generic relations of this species are still quite an open question. 
 Moore’s description and figure do not throw any light upon them. 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 Order—LUCIN ACEA, 
 Family—LUCINIDZ. 
 
 Genus—CORBICELLA, Lycett, 1857. 
 (Handb, Cotteswold Hills, p. 128.) 
 CoRBICELLA ? MARANOANA, sp. nov. 
 Pl. 27, figs. 4 and 5; ? Pl. 28, figs. 2 and 3. 
 Sp. Char. Shell elongately oval, rather pod-shaped, with a slight obliquity to 
 the posterior, almost equilateral ; valves gently convex; not inflated nor gibbous ; dorsal 
 
 * Dumont D’Urville’s Voy. au Pole Sud Geolozie, Atlas, 1847, t. 7, f. 31. 
 
472 
 
 margin long, nearly straight; ventral margin rounded at either end, almost straight 
 along the centre. Anterior end nearly equal to the posterior, the roundly truncate 
 margin obliquely curved upwards, giving to the shell the described obliquity, the 
 posterior only differentiated by its greater length. Umbones nearly central. Dorsal or 
 hinge margin thickened with an anterior cardinal tooth, large, solid, and somewhat 
 triangular, posterior cardinal tooth but little developed. Concentric lines of growth 
 very regularly follow the outline, turning sharply towards the umbones on the anterior 
 slopes, and curving rather obliquely up on the posterior end, but the shell is in reality 
 nearly smooth. 
 
 Obs. This shell has given more trouble in its determination than any other in 
 the whole Collection, and is referred to the present genus with great doubt ; itis probably 
 the type of an undescribed genus. In Pl. 27, fig. 4, the anterior end has been broken 
 away, and on that account much of the anterior obliquity is lost, but this is apparent in 
 Pl. 28, fig. 2, which, I believe, is only the internal cast of Corbicella maranoana. This 
 peculiar obliquity towards the posterior recalls the genus Cercomya to some extent, but 
 there is an entire absence of the strong diagonal ridge and posterior slope of that genus. 
 The upturning of the posterior dorsal margin arises from a peculiarity of the cast, and 
 is perhaps structural, being probably the edge of the interior of the valves below the 
 thickened hinge plate. It may, perhaps, be doubted if Pl. 28, f. 2 and 3, are the 
 internal cast of Pl. 27, fig. 4, but there is a depression beneath the beaks in an example 
 of the former answering to that visible in Pl. 27, fig. 5, and, as already explained, the 
 anterior end of Pl. 27, fig. 4, is a good deal broken away. This species exists in Prof. 
 Tate’s Collection from South Australia, and is termed by him Poromya, but it does not 
 coincide with the original type of that genus. Prof. Tate’s specimens and others from 
 the cabinet of Mr. G. Sweet will eventually be figured. 
 
 After considerable hesitation I provisionally refer this peculiar shell to 
 Lycett’s genus Corbicella, from the fact that the structure of the hinge seems to agree 
 better with that of the latter than with any other genus. The shell may readily be 
 known by its ovoid, lengthened, smooth form. In these particulars, more especially 
 the two last, it has considerable resemblance to some Oolitic species of Corbicella, but in 
 the case of a shell like the present, in which the hinge is only partially preserved, it is 
 necessary to speak with caution. 
 
 Loe. Maranoa River, half a mile above Mitchell Railway Station, in a core of 
 limestone (R. L. Jack; G. Sweet—Colln. Sweet, Melbourne). 
 
 Genus—UNICARDIUM, D Orbigny, 1850. 
 (Prod. Pal. Strat., i., p. 218.) 
 
 UnicarpiumM MEEKI, sp. nov. 
 
 Pl. 27, figs. 2 and 3; ? Pl. 26, figs. 18-15. 
 
 Sp. Char. Shell gibbous, ovate-trigonal; cardinal margin angular; umbones 
 obtuse, a little elevated, with the beaks close and approximate. Anterior side rounded, 
 somewhat produced; posterior end produced, becoming rather pointed at the posterior 
 ventral angle; posterior slope flattened; ventral margin forming a broad semi-oval 
 curve. Anterior muscular scar narrow-ovate, pointed above, with its posterior margin 
 elevated and ridge-like. Pallial line indistinct; surface marked with fine lines of 
 growth, which appear to widen out into flatter ridges on the body of the shell. 
 
473 
 
 Obs. It was not until I had examined Prof. Tate’s Collection of South Australian 
 Cretaceous fossils that I was able to make out the generic relations of this species, 
 through a knowledge of the internal hinge characters, having previously referred the 
 type (Pl. 27, figs. 2 and 3) to the genus Mactra. 
 
 In the left valve of U. Meeki the conical cardinal tooth is well marked and 
 prominent, with a deep socket on its posterior side for the reception of the tooth of the 
 right valve. 
 
 Unicardium cardioideum, Phillips,* has similar wide concentric lines of growth to 
 the present species. 
 
 In a future publication the hinge structure of this species will be figured. 
 
 Loc. Waish River (Hon. A. C. Gregory). 
 
 Order—VENERACEA. 
 Family—VENERIDZ. 
 
 Genus—CYTHEREA, Lamarck, 1806. 
 (Ann. Mus. Hist. Nat. Paris, vii., p. 132.) 
 
 CyruErEA Woopwarpiana, Hudleston, Pl. 27, figs. 12-14. 
 Cytherea Woodwardiana, Hudleston, Geol. Mag., 1884, i., p, 340, t. 11, f. 8a-c. 
 
 Sp. Char. Shell oval, compressed, veneriform, longer than broad. Hinge-line 
 inclined on both sides; dentition unknown ; umbones small, quite approximate; lunule 
 almost imperceptible, nearly flat; ligament small, but prominent. Ventral margin 
 regularly rounded. Anterior end small, the margin gracefully rounded; posterior end 
 rather more produced than the anterior. Pallial sinus large, and much sinuated for so 
 small a shell, the first turn from the anterior towards the posterior end, forming a very 
 sharp angle. Surface with about five broad, concentric, flat undulations, between which 
 are very fine close striw, having a similar direction, and the whole crossed by fine 
 radiating strie. 
 
 Obs. I cannot agree with Mr. W. H. Hudleston in saying that the radiating 
 striz are irregular. On the examples examined these lines were quite normal. This 
 character and the compressed nature of the valves are excellent features for the 
 determination of the species. On removal of the outer shelly layer, the radiating striz, 
 it is true, quite disappear. 
 
 The inflection of the hinge calls to mind the structure of the genera Cyprimeria 
 and Oaryatis, rather than that of a true Cytherea, especially such species as Cyprimeria 
 gaultina, Loriol.+ © 
 
 CyTHEREA? HupLEsTonl, sp. nov., Pl. 28, fig. 12. 
 
 Sp. Char. Shell ovately trigonal, rather acuminate towards the umbones, tumid ; 
 body of the shell convex, which is more or less maintained to the ventral margin, not 
 thinning away rapidly to the latter ; hinge margin much arched; ventral margin 
 rounded ; posterior margin slightly angulated; posterior slope broad and rounded ; 
 surface with regular, concentric, sub-imbricating lamine. 
 
 Obs. A very obscure shell, not easily defined, but important as forming con- 
 siderable rock masses, associated with Acteon depressus, Moore?, Oucullea Henderson? 
 (mihi), Dentaliwm, and other shells. 
 
 The nature of the hinge is unknown, and the shell does not possess any very 
 distinctive characters beyond its shape. It is an undoubted specific addition to the 
 
 * Til. Geol. York., 3rd Edit., Part i., 1875, t. 14, f. 12. 
 + Mém. Soc. Pal. Suisse, x., p. 35, t.7, f. 1-5. 
 
474: 
 
 Australian Mesozoic list, and I have much pleasure in associating with it the name of 
 Mr. Hudleston, whose labours amongst the Secondary Mollusca are much appreciated. 
 It is provisionally placed in Cytherea at the suggestion of Mr. J. Brazier. 
 
 Loc. North-east end of Glanmire Block, seventeen miles south-west of Tambo 
 (Mr. Goffage). 
 
 Cyruerra (Cyprtna?) Moorst, sp. nov., Pl. 34, figs. 12 and 13, 
 Cyprina ? sp., Hudleston, Geol. Mag., 1884, i., p. 341, t. 11, f. 7a and b. 
 
 Sp. Char. Shell ovate, width and length nearly equal, hinge-line or cardinal 
 margin sloping sharply on both sides; ventral margin regularly rounded, anterior end 
 short ; posterior end obtusely pointed. Lunule probably long and moderately deep. 
 Umbones but little incurved; umbonal region obtuse, the test much thickened thereabouts; 
 flanks compressed towards the ventral margin. Sculpture of surface unknown. 
 
 Obs. I am unacquainted with the nature of the hinge, thus leaving the question 
 of its generic position, whether Cytherea or Cyprina, an open one. An examination 
 of Mr, Hudleston’s type showed that the “concentric bands at intervals’’ are simply 
 eroded layers of shelly matter, the surface, in all probability, having been comparatively 
 smooth. Both the original descriptionand figure are therefore in this respect misleading, 
 The preservation of the type certainly does not permit of it being said—lunule wide 
 and deep, ligamentary excavation wide and short,” for these portions of the specimen 
 are notin acondition favourable for description. Thelunule was long, but not particularly 
 deep. . ; : 
 
 A specimen (Pl. 26, figs: 11 and 12) has been presented to the Queensland 
 Geological Survey Collection by Mr. Rowland Morrisby, which appears to correspond 
 closely with Mr. Hudleston’s species, but it presents a slightly different aspect on 
 account of the preservation of the umbo, which gives the specimen a rather higher and 
 less robust appearance. ; 
 
 Loc. Evora Station, twenty-five miles north-east of Blackall (2. Morrisby) ; 
 Peak District, South Australia (A. ¥. L. Brown—Nat. Hist. Museum, London)—Lake 
 Eyre Beds. 
 
 Family—CY PRINIDA. 
 
 Genus—CYPRINA, Lamarck, 1818.* 
 (Hist. Anim. sans Vertéb., v.) 
 
 Cyprina CiarKer, Moore, sp. 
 
 Pl. 27, fig. 9; P Pl. 26, figs.-18 and 19; ? Pl. 27, figs. 10 and 11. 
 
 Cytherea Clarket, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 250, t. 13, f. 1. 
 Cyprina expansa, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 338, t. 19, f. 1. 
 
 Sp. Char. Sheil large, thick, rather compressed, transversely ovate, inequilateral, 
 moderately convex; umbones flattened, incurved over a large and rounded lunule; 
 anterior and posterior ends and dorsal margin rounded; surface of the shell with broad 
 irregular transverse bands of growth. (dfoore.) 
 
 Obs. Unfortunately Mr. Moore’s description of this important shell is most 
 inadequate for its correct determination, and the figure is little better. As represented, 
 it would convey to the eye the idea of a shell possessing a very concave anterior hinge, 
 and a much arcuated and obliquely directed posterior hinge-line. Along the latter line, 
 however, the specimen figured was clearly defective. During a comparatively recent 
 
 
 
 * Probably proposed in 1812, in the ‘‘ Cours de Zoologie.” 
 
475 
 
 conversation with Prof. R. Tate, he expressed the opinion that this species was identical 
 with Cyprina expansa, Etheridge. It is, of course, extremely difficult to arrive ata definite 
 conclusion when dealing with such imperfect material, and when also the types are not 
 before us; but, allowing for discrepancies of outline, I find myself quite in accord with 
 so authoritative an opinion. In Cyprina expansa the umbones are quite anterior, and 
 projecting forwards prominently ; the curve of the anterior hinge from the umbones is 
 short, and the posterior hinge-line more or less horizontal, giving to the shell, with 
 its other features, a somewhat quadrangular aspect. On the other hand, in Cytherea 
 Clarkei the umbones are some way removed from the anterior end; the curve of the 
 anterior hinge is long and open; whilst the posterior hinge rapidly descends in an 
 oblique curve, although, as before stated, this portion of Moore’s specimen was clearly 
 defective. At any rate, this is the view the appearance of the figures would appear to 
 justify. 
 
 More closely resembling Moore’s figure are those given on our Plate 27 (figs. 10 
 and 11), although representing a smaller shell. The specimens are of medium size, 
 rotund-ovate, longer than high, and with no great convexity of valves. The hinge was 
 arcuate, especially on the posterior side, and the ventral margin well rounded ; umbones 
 moderately convex and close together, incurved, and rather more anterior than posterior. 
 The muscular impressions are well marked, especially the anterior, whilst the pallial 
 line was deeply and widely sinuated. Portions of the shell are preserved showing that 
 the surface bore fine regular, raised, concentric lines, here and there broken by a more 
 marked interruption of growth, and on the anterior end crossed by a few oblique 
 similar lines, but not on other portions of the test. 
 
 If the two shells (Pl. 27, figs. 10 and 11) are not Cytherea Clarkei, I am at a loss 
 as to their identity, and can only arrive at the conclusion that they are an unnamed 
 species of Cytherea, so far peculiat to the Queensland beds. The less transversely 
 elongated and arcuate outline will distinguish them from the species here called 
 Macrocallista Taylori. Cytherea Clarkei evidently attains a considerable size. “It is 
 one of the largest of Australian bivalves,” says Mr. Moore, “‘ and appears to have attained 
 a large size, even for a Cytherea. . . . . The largest example measures six and 
 a-quarter inches in breadth by four and a-quarter inches in depth.” 
 
 In addition to this species Mr. Moore alluded to a second, under the name of 
 Cytherea gibbosa, with the following brief remarks :—‘‘ A second species, much more 
 convex and gibbous, with umbones much thickened, is present, but the specimen is too 
 imperfect for description. It is from Wollumbilla.” This was not figured, and as it is 
 impossible to recognise a species from such a description, the name had better be 
 expunged from the list. 
 
 Loe. Wollumbilla (The late Rev. W. B. Clarke); Maranoa River (Zdid.) ; 
 Gregory River, north of Finnis Springs (Zbid.); Upper Flinders River (Hon. A. C. 
 Gregory) ; Walsh River, Pl. 27, figs. 9 and 11 (Hon. A. C. Gregory) ; Minmi, near 
 Roma (#. Z. Jack). Also recorded by Prof. R. Tate,* from Cootanoonna, thirty or 
 forty miles north-west of the Peake, Central Australia, and from the Peake. 
 
 Genus—CALLISTA, Poli, 1791. 
 (Test. Utr. Sicil.) 
 Section—MACROCALLISTA, Meek, 1876. 
 (invert. Cret. and Tert. Foss, Up. Missouri Country, p. 179.) 
 Obs. It is more than probable that this section of Callista exists in the Queens- 
 land Cretaceous. The excellent remarks of the late Mr. Meek in reference to the proper 
 
 * Trans. R. Soc. 8. Austr. for 1879-80 [1880], iii:, p. 179. 
 
 
 
476 
 restriction of Poli’s genus, as typified by Venus chione, Linn., will prove to be of great 
 assistance to all workers. Dacrocallista was proposed by Meek to include forms 
 resembling Venus gigantea, Gmelin. The shell is transversely elongate-oval, with a 
 
 more or less smooth surface. The pallial sinus is deep, resembling that of Callista 
 proper, but the details of the hinge differ to some extent. 
 
 Macrocatiista PLaNa, Moore, sp., Pl. 27, figs. 6-8. 
 Myacites planus, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 254, t. 12, f. 10. 
 
 Sp. Char. Shell transversely elongated, somewhat compressed, length one 
 and three-quarters that of the height ; anterior end rounded and narrowed; posterior 
 side elongated and pointed ; dereal margin gently curved posterior, to the umbones ; 
 ventral margin forming an open free curve ; umbones subcentral, nearer the anterior end ; 
 muscular impressions round or oval, usually well marked; pailial sinus very deeply 
 indented. Surface nearly smooth, with very fine concentric lines of growth, becoming 
 broader towards the ventral margin; character of the hinge, lunule, and escutcheon not 
 ascertained. 
 
 Obs. I have been unable to satisfactorily refer this shell to any known genus of 
 Cretaceous Bivalves, from the obscure preservation of the hinge and teeth. An internal 
 cast shows that it possessed both cardinal and lateral teeth, apparently after the type 
 of the Veneride, but more than this cannot be said. In outward appearance the shells 
 closely resemble those which Mr. Meek has proposed to separate as Macrocallista, but 
 the umbones are rather too tumid, and hardly project far enough forward. The species 
 is not allied to any of those referred to Callista by Stoliczka from the Indian Cretaceous 
 series. On the other hand, it has much the appearance of a shell called yacites by 
 Mr. R. Etheridge, }'.R.S.,* from the Gordon Downs. The shell in question is not a 
 Myacites ; it has no characters in common with that genus, and of this Mr. Etheridge 
 is himself now satisfied. In all probability it is the species under description, and as 
 to the horizon stated—viz., Lower Oolite—the beds in which the fossil was found 
 certainly form a portion of the ‘‘ Rolling Downs Formation.” Reference may be made 
 in passing to Myacites planus, Moore, from Wollumbilla, which presents a resemblance to 
 our shell, but is perhaps shorter from side to side, the former being longer in proportion 
 to its width. The Collection contains other imperfect and unnameable casts which 
 may, perhaps, be referable to the present genus, but absolute Cortolaby cannot a 
 affirmed. 
 
 Judging from Moore’s figure, Ayacites planus does not appear to be congeneric 
 with those on which Schlotheim established the genus Myacites. 
 
 Loc. Walsh River (Hon. A. O: Gregory); Wollumbilla (Zhe late Rev. W. B. 
 Clarke). 
 
 Family—CARDIIDZ. 
 
 Genus—LEVICARDIUM, Swainson, 1840. 
 (Malacology, p. 3738.) 
 
 L2&VICARDIUM BRAZIERI, sp. nov.t 
 Sp. Char. Shell large, ovate, convex and gibbous, almost equilateral; test 
 thick ; dorsal margin short, curved; umbones nearly central, gibbous; anterior and 
 posterior ends almost equal, but the latter a little more produced, their margins and 
 that of the ventral round, and running into one another ; anterior slope rather flattened, 
 
 
 
 * Quart. Journ. Geol. Soc., 1872, xxviii, p. 348. 
 + This shell will be figured in a Supplement to the present Work. 
 
477 
 
 posterior hardly developed; general contour from the umbones to the ventral margin, 
 convex and well rounded. Surface smooth, with the exception of very delicate, scarcely 
 defined, concentric lines, more apparent towards the ventral margin, and there are the 
 feintest indications of radiating lines, more marked on the anterior and posterior 
 sides. 
 
 Obs. This large and well-marked shell was communicated by the late Rev. 
 J. E. T. Woods, and although the locality has been mislaid it is unquestionably a 
 Queensland shell. It is in a shelly limestone associated with a large number of 
 Nucule. 
 
 The nearly central position of the beaks and oval outline give it a very equilateral 
 appearance, added to which the practically smooth surface renders it a species not 
 easily forgotten. The dental characters are unknown, but were probably powerful, 
 judging from the thick and strongly made shell. The radiating ribs would hardly be 
 worthy of notice were it not that, when the test is weathered these appear in its 
 substance very distinctly, and when crossed by the fine concentric lines break up the 
 shelly matter into small quadrangular spaces, as frequently seen in some of the 
 Cardiidee. 
 
 The only species I can at all compare with the present one is Cardiwm 
 imbricatarium, Leymérie, as figured by Hichwald.* The shape is the same, and there is 
 a resemblance in the absence of sculpture and radiating ribs, although the last-named 
 species has three along the position of the posterior slope. In our species the 
 concentric lamine are very fine and close together, but in Leymérie’s species they are 
 broad and somewhat distant. 
 
 The exact locality has been mislaid, but Mr. Woods informed me that it was 
 without doubt collected in Queensland. 
 
 It is named in honour of Mr. John Brazier, C.M.Z.S., Conchologist to the 
 Australian Museum, to whom the Writer is indebted for cheerfully rendered assistance. 
 
 Loc. Queensland (The late Rev. J. H. T. Woods—Colln. Woods). 
 
 Family—DONACIDZ. 
 
 Genus—TANCREDIA, Lycett, 1850. 
 (Ann. and Mag. Nat. Hist., vi., p. 407.) 
 
 Obs. Two Australian Mesozoic shells have been referred to this very well- 
 marked genus, Zancredia plana, Moore, and Tancredia, sp. ind. (Etheridge). They are so 
 retained in deference to the opinion of such well-known Authorities in Secondary Paleon- 
 tology, although neither shell corresponds in outward appearance with the type species of 
 Tancredia, T. donaciformis, Lycett, or with the next described form Z. extensa, Lycett. 
 The hinge characters of the Australian shells are not known. 
 
 TANCREDIA P PLANA, Moore. 
 Tancredia plana, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 254, t. 18, f. 13. 
 Sp. Char. Shell thin, smooth, flattened, transversely ovate, rather inequivalve ; 
 anterior side rounded ; posterior margin oblique; surface of the shell covered by very 
 
 fine transverse striations. (Jloore.) 
 Loc. Blythesdale, fifteen miles from Wollumbilla (The late Rev. W. B. Clarke). 
 
 * Lethea Rossica, ii., p. 682, t. 25, f. 11. 
 
478. 
 
 TANCREDIA ? sp. ind. 
 Tancredia, sp.? Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 348, t. 25, f. 8. 
 
 Obs. Mr. R. Etheridge, F.R.S., compared this shell to Corbicella bathonica, 
 
 Morris and Lycett, an indication which appears to be strongly in favour of its reference 
 
 to that genus rather than to Tuncredia. So far as the mere outline is concerned, it may 
 
 be compared in passing to Macrocallista plana, Moore, sp., and even Mr. Etheridge’s 
 
 Myacites, sp.; in fact, the figure of the latter and the Zancredia are remarkably alike. 
 Loc. Gordon Downs (The late R. Daintree). 
 
 Order—TELLINACEA. 
 Family —TELLINID®. 
 
 Genus—PALAOMARA, Stoliczka, 1870. 
 (Pal. Indica (Cret. Fauna), 1870, iii., fase. 1-4, p. 116.) 
 
 PAaLEoMmRA ? sp. ind., Pl. 26, fig. 16. 
 
 Obs. A very interesting shell, probably referable either to this genus, or Tellina, 
 has come to light through the sinking of the Muttaburra Well. Only one valve is 
 extant, and both the extreme ends are destroyed. The valve could only have been 
 moderately convex, the posterior slope but little developed. On the other hand, the 
 umbo was acute and sharp, small and incurved, whilst fine concentric lines ornamented 
 the surface. By prolonging the concentric strie, the length, when perfect, would be 
 about an inch and a-quarter. 
 
 The present shell to some extent resembles a Psammobdia, although not of the 
 typical form. It also reminds one of TZellina equalis, Gabb.,* of the Californian 
 Cretaceous Beds. 
 
 Loc. Bore at Muttaburra (J. B. Henderson). 
 
 Genus—GLYCIMERIS (Klein), Lamarck, 1799. 
 
 Glycimeris (Klein), Lamarck, Mem. Soc. Hist. Nat. Paris, 1799, p. 83 [non Lamarck, 1801, Syst. Anim. 
 sans Vertéb, p. 126 = Cyrtodaria, Daudin]. 
 Panopea, Ménard de Ja Groye, Ann. Museum Hist. Nat. Paris, 1807, ix., p. 185. 
 Obs. Observations on this genus will be found under the head of “ Desert 
 Sandstone,” to which the reader is referred. 
 
 GuyrcrmeErts ruGosA, Moore, sp., Pl. 28, figs. 4 and 5, ? fig. 6. 
 
 Panopea rugosa, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 253, t. 18, f. 7. 
 Myacites? australis, Hudleston, Geol. Mag., 1884, i., p. 340, t. 11, f. 9. 
 
 Sp. Char. Shell transversely ovate, anteriorly inflated, very convex cr gibbous 
 in the umbonal or visceral region. Dorsal margin straight (with a raised ridge for 
 ligamentary attachment, J/oore); ventral margin rounded at the ends, almost straight 
 in the centre. Anterior end closed, somewhat produced, with a sub-truncate margin 
 and an anterior slope rather angulated from the umbones forward; posterior end 
 rounded, more or less gaping along the posterior dorsal margin. Umbones incurved, 
 acute (Moore), depressed or flattened from above. Pallial sinus very deep and 
 moderately wide; anterior muscular impressions faint, posterior well marked. Surface 
 with irregular, rough, concentric ruge, stronger on the anterior end, with an epidermal 
 covering of anastomosing fibres. 
 
 
 
 
 
 * Pal. California, 1869, ii., p. 182, t. 29,.f, 73, 
 
479 
 
 Obs. G. rugosa is a very wide-spread and typical shell, as not only does it occur 
 at several localities in Queensland, but I have it in Prof. Tate’s South Australian 
 Collection. Moore’s figure is most unsatisfactory, and generally unlike the shell, but 
 possessing specimens from the typical locality, and not having seen any-other shell so 
 nearly corresponding with his species, I believe the determination to be correct. The 
 hinge structure has not been satisfactorily made out, while it seems to be a shorter and 
 broader form than Moore’s Mya Maccoy?, although the latter is not definitely known 
 to me. 
 
 Glycimeris rugosa seems to be distinguished from G. suleata, Etheridge, by its 
 more robust habit and the less rugged condition of the concentric undulations. One 
 of the most striking features of G. rwgosa is its anterior inflation, but I think the 
 anterior margins are closed, in which case the species departs somewhat from the generic 
 diagnosis of Glycimeris, Klein (Panopea, Ménard). The concentric undulations on the 
 umbones are particularly regular and close. 
 
 Prof. T. W. E. David has collected an internal cast at Maryborough,* which 
 appears to be too large a shell for G. sulcata, Etheridge, and may indicate the presence 
 of the present species at that locality. 
 
 A striking resemblance exists between this species and Mr. Hudleston’s 
 Myacites ? australis, which, it is almost needless to say, has no relation to typical] 
 species of that genus. There are the same prominent umbones, square anterior end, 
 and rather attenuated posterior end, and when seen ina side view the likeness is very 
 marked. It must be admitted, however, that G. rugosa has a more geuerally solid 
 appearance, and isa broader shell across the valves. Although Myacites ? australis 
 cannot be described as a compressed form, still its girth is less in proportion to size 
 than in the present species. Notwithstanding these differences, I do not think that the 
 one can be regarded as more than a compressed variety of the other. 
 
 Mr. Hudleston drew attention to the general resemblance of his species to the 
 Shells figured by Mr. Etheridge as Panopea sulcata, but, although generically allied, 
 there is no specific relation. 
 
 Loe. and Horizon. Bungeworgorai Creek, near Mount Abundance (The late 
 Rev. W. B. Clarke) ; Maranoa River, half a mile above Mitchell Railway Station, Pl. 28, 
 figs. 4 and 5 (R. L. Jack) ; Maranoa River and Wollumbilla (G. Sweet—Colln. Sweet, 
 Melbourne). 
 
 Myacites? australis was obtained in the Peak District, South Australia, 
 and forty-five miles south-west of Cootanoonna Station, Lake Hyre (Hl. ¥. L. Brown— 
 Nat. His. Mus., London). 
 
 ? Occurs also in the Maryborough Beds (yecert Sandstone) (1. W. #. David— 
 Colln. David, Sydney). 
 
 GLYCIMERIS ARAMACENSIS, sp. nov., Pl. 28, figs. 7 and 8. 
 
 Sp. Char. Shell small, transversely elongated and a little oblique, gaping at both 
 ends, somewhat compressed. Anterior end small, the margin rounded; posterior end 
 slightly attenuated, the margin apparently rounded, and to some extent truncate ; 
 ventral margin sharp and nearly straight. Umbones much incurved, obtusely flattened 
 from above; posterior slopes small, flattened; diagonal ridges acute, especially towards 
 the umbones. Anterior slopes very short and wider than the posterior; shell probably 
 thin. Surface with coarse, large, and almost rugged concentric undulations, fourteen to 
 
 
 
 * Maryborough Beds—Desert Sandstone, 
 
480 
 
 fifteen in number, smaller and more numerous ov the umbones, gradually widening out 
 on the body of the shell, and very widely separated on the posterior ends; between the 
 undulations are delicate strie. 
 
 Obs. The coarseness of the concentric undulations brings this shell in close 
 relationship with Glyeimeris sulcata, Eth., but it is much longer in proportion to its 
 height than that species, with a longer anterior end, and a straighter hinge. 
 
 Loc. Aramac (&. L. Jack). 
 
 Guycrmeris ? Maccoyr, Moore, sp. 
 Mya Maccoyi, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 253, t. 13, f. 8. 
 
 Sp. Char. Shell ovately oblong, moderately large, tumid, inequivalve ; umbones 
 anterior, incurved, close ; anterior margin truncated, angular ; posterior end attenuated, 
 rounded, widely gaping ; ventral margin slightly rounded ; surface of the shell with wide 
 irregular lines of growth, the outer surface of the test, where best preserved, showing 
 itto be very wrinkled. Itis three and a-quarter inches broad by two and a-quarter in 
 height. (oore.) 
 
 Loc. Between the Amby and Maranoa Rivers (The late Rev. W. B. Olarke). 
 
 Family—ANATINIDA. 
 
 Genus—GONIOMYA, L. Agassiz, 1842. 
 (Etudes critiques Moll. Foss. 2e Livr., p. 1.) 
 
 GONIOMYA DEPRESSA, Moore, Pl. 28, fig. 9. 
 Goniomya depressa, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 251, t. 13, f. 6. 
 
 Sp. Char. Shell ovately elongated, thin, flattened; umbones close, depressed, 
 mesial ; anterior end rounded; the middle of the valves with a depression or fold from 
 the umbo, which widens to the ventral margin, surface with broad curved rounded 
 cost. (Moore.) 
 
 Obs. The posterior end of this figure, copied from Mr. Moore’s illustration 
 (Pl. 28, fig. 9) is wanting. 
 
 The genus Goniomya made its first appearance in the Lias, but did not survive 
 the Cretaceous Period. 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Genus—HOMOMY A, Agassiz, 1842. 
 (Etudes critiques Moll. Foss., 3¢ Livr. p. 154.) 
 
 Homomrya, sp. ind. 
 Homomya, sp., Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 347, t. 25, f. 5. 
 
 Obs. Two specimens of this genus, in a micaceous sandy or arenaceo-calcareous 
 limestone, were examined by Mr. R. Etheridge, F.R.S., who remarked—* The absence 
 of radiating cost, and the somewhat wrinkled surface of the shell, as well as the position 
 of the umbo and the gently curved hinge-line, favour the view that the two casts belong 
 to the genus Homomya.”’ 
 
 Loc. Gordon Downs (Thelate R. Daintree). 
 
481 
 
 Genus—CORIMYA, L. Agassiz, 1842. 
 (Etudes critiques Moll. Foss., 3¢ Livr., p. 262.) 
 
 Cortmya Wrusont, Moore, sp., Pl. 28, figs. 10 and 11. 
 Thracia Wilsoni, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 254, t.14, f. 8. 
 
 Sp. Char. Shell transversely ovate, thin, compressed, especially towards the 
 posterior ventral margin, slightly inequivalve. Hinge-line slightly concave anteriorly, 
 and the same, or horizontal, on the posterior; ventral margin rounded ; internally the 
 upper of the posterior ribs is placed close under the hinge-line, and almost parallel to 
 it, but the lower bounds the posterior slope, and is oblique. Anterior side shorter 
 than the posterior; the latter is somewhat produced, and sub-truncate ; posterior slope 
 slight; diagonal ridge rounded and inconspicuous. Umbones nearly median, but nearer 
 the anterior end. Surface with concentric growth-lamine and strie, all becoming 
 stronger on the posterior end. 
 
 Obs. The shell represented in Pl. 28, fig. 10, is Mr. Moore’s type, and this 
 figure, of the natural size,.may be taken as a sample of the unreliable nature of his 
 illustrations of the Queensland fossils generally. It is preserved in the Museum of 
 the Literary and Philosophical Society of Bath, and I am indebted for the loan of it to 
 the kindness of the Committee of that Institution through the Rev. H. H. Winwood, 
 M.A. 
 
 This fossil has the shell preserved, but in fig. 11 of the same plate is what I 
 believe to be the internal cast of another species. The two grooves under the posterior 
 hinge naturally represent shelly ribs on the interior of the valve, and correspond to 
 the structure of Agassiz’s Corimya, especially as there is no trace of hinge teeth, or 
 other features, which would invalidate the reference, such, for instance, as the 
 cartilage pit of Anatina. It is probably Mr. Hudleston’s Thracia primula,* from South 
 Australia. 
 
 Mr. Moore mentions the existence of an external ligament, and describes the 
 valves as unequal, through the presence of “a slight sinus towards the centre of the 
 
 ventral margin, with a corresponding elevation on the opposite valve.” The possession 
 
 of a ligament by this species would support Stoliczka’s view that Corimya was furnished 
 with such a mechanism. The inequality of the valves I have not seen. 
 
 Loc. and Horizon. Amby River and Bungeworgorai Creek (The late Rev. W. B, 
 Clarke) ; Mimni, near Roma (R. L. Jack). 
 
 Family—MACTRID. 
 
 Genus—MACTRA (Linn.), Lamarck, 1799. 
 (Mém. Soc. Hist. Nat. Paris, 1799, p. 85.) 
 
 Maorra TRIGONALIS, Moore, Pl. 27, fig. 17. 
 
 Mactra trigonalis, Moore, Quart. Journ. Geol. Soc., 1872, xxvi., p. 252, t. 14, f. 6. 
 Sp. Char. Shell small, thin, trigonal; umbones rather anterior; anterior end 
 rounded and rather angular; front margin rounded; the surface is marked by faint 
 
 transverse lines. (Joore.) 
 Loc. Nive River Downs (The late Rev. W. B. Clarke). 
 
 9 * Geol, Mag., 1890, vii. (3), p, 245, t. 9, £. 7. 
 @ 
 
482 
 
 Order—PHOLADACEA. 
 Family—G ASTROCH EZ NID. 
 
 Genus—GASTROCH ANA, Spengler, 1783. 
 
 Gastrochena, Spengler (Lamarck partim), Saml. Kongl. Danks. Vid. Selsk. Skr., ii., p. 174. 
 Chena, Phillipsson in Retzius, Dissertatio Hist. Nat., 1788, p. 19. 
 
 GASTROCHENA AUSTRALIS, sp. nov., P]. 31, figs. 6-8. 
 
 Sp. Char. Valvesunknown. Tube tapering but little in the fragment preserved, 
 section nearly round. Surface covered with very fine anastomosing lines, which are 
 the broken off, or rubbed down edges of a series of shelly frills, forming by their 
 anastomosis transversely elongated spaces. 
 
 Obs. This object for a long time defied determination, but I believe the shell 
 structure of the living Gastrochena grandis, Desh., will explain its nature. 
 
 In the tube of the recent species the structure of the outer layer is vesicular, 
 arising from the mechanical union of frilled surfaces with particles of sand. If this 
 vesicular structure be broken, or worn-down, a series of anastomosing frills or ridges 
 are formed, enclosing vesicles or chambers, usually transversely elongated. Supposing 
 these to be still further denuded, the resulting structure would be a series of 
 anastomosing lines on the fossil, instead of frills. Such is, I believe, the origin of 
 those seen on the specimen now under description. 
 
 A species has been described from the Cretaceous rocks of India, but it is 
 quite different from the above. 
 
 Loe. Maranoa River, half a mile above Mitchell River Station (2. L. Jack). 
 
 PELECYPOD INCERT SEDIS. 
 
 Obs. Under this heading are placed a few-bivalves which it has been found 
 impossible to relegate to their proper genera. ‘They are figured, or refigured, as the 
 case may be, in the hope that attention may be called to them, and additional 
 examples obtained for further elucidation. 
 
 Pu. 21, Fra. 15.—A somewhat rectangular valve, with the umbo quite at the 
 anterior end, a nearly straight cardinal margin, and but little convex surface, which is 
 marked with a few concentric lamine. The posterior margin appears to be slightly 
 emarginate. Under it is another individual, which may be the opposite valve of the 
 same species, bearing six rib-like costz, and shorter intermediate ones. 
 
 Loc. Aramac (R. L. Jack). 
 
 Pu, 21, Fra. 16.—A nearly flat meleagriniform valve without any anterior ears, 
 an inconspicuous umbo, short cardinal margin, slightly emarginate posterior margin, 
 and indistinct concentric lines. This bears a striking resemblance to left valves of 
 Whitfield’s genus Meleagrinella,* and which it may even represent, but I have not seen 
 any corresponding right valves possessing the peculiarities of that genus. It is like 
 M. abrupta, Conrad, sp.t, and to some extent MW. curta, Wall, sp.t Some resemblance is 
 also borne by ouxg shell to the Indian Cretaceous species Pseudomonotis inops, Stoliczka. 
 
 Loc. Aramac (R. L. Jack). 
 
 Pr. 21, Fre. 14.—A bivalve of a somewhat similar type to the above, but too 
 indistinct and imperfect to have much stress laid upon it. The umbo is much more 
 median, and the ornament is concentric. 
 
 Loc. Coreena Woolshed (R. L. Jack). 
 
 * Mon. U.S. Geol. Survey (Powell’s), 1885, ix., p. 71. 
 
 + Whitfield, loc. cit., t. 14, f. 11. 
 
 £U.S. Geol. Survey Rocky Mt. Region (Powell’s), Whitfield’s Pal. Black Hills of Dakota, p. 354, 
 t, 3, f. 20, 
 
 
 
 
 
 
 
 
 
483 
 
 Pu. 24, Fra. 1.—In this figure is represented a much compressed right valve of 
 a Maccoyella-like bivalve. There are no traces of radiating coste, but in their place 
 strong concentric lines and lamine. The dorsal margin was clearly straight, the 
 anterior end much cut out and projecting ventrally, the ventral margin very regularly 
 rounded, and the beak small and depressed. The shell structure is that of Maccoyella. 
 
 Loc. Flinders River, three miles above Richmond Downs Station (R. L. Jack). 
 
 Pr. 26, Fre. 13-15.*—It has been found impossible so far to identify the genus 
 of this shell, notwithstanding that it has been very carefully considered both by 
 Prof. R. Tate, Mr. J. Brazier, and myself, owing to our want of knowledge of the 
 pallial line and the hinge-structure of the right valve. The shell is obliquely 
 trigonal, tumid in the umbonal region, the posterior end small and rather acumi- 
 nate. The hinge or cardinal margin is strongly angulated, descending rapidly on 
 the posterior side, but less so on the anterior. The ventral and anterior margins 
 are rounded; body of the shell gibbous, and somewhat inflated, with well incurved 
 umbones. The shell possesses an inconspicuous and not well defined lunule, aud there 
 is no defined siphonal ridge. The ligament was external. The dental characters, so 
 far as known, in the left valve are very marked, consisting of a large projecting 
 ‘somewhat triangular cardinal tooth with a deep socket immediately on its posterior 
 side, and an elongated lateral tooth. It may be a Unicardium. ‘The only shell 
 described by Moore which could have any relation to this species is his Astarte 
 wollumbillensis, but the figare being only a partial one is quite useless for comparison. 
 
 Loe. Upper Flinders River (Hon. A.C. Gregory). 
 
 Pu. 26, Fras. 11 and 12.—A cytheriform shell, the valves united and much 
 decorticated, several layers having flaked off. The hinge is not visible, but there 
 appears to have been a lunule and an escutcheon. The outline of the valves would 
 indicate a genus near Cytherea or one of itsallies. There is some resemblance to Cytherea 
 (?) Hudlestont (Pl. 28, fig. 12). 
 
 Loc. Evora Station, twenty-five miles north-east of Blackall (Ze. Morrisby). 
 
 Class—G-ASTEROPODA. 
 
 Order—SOLENOCHONCHA. 
 Family—DENTALIIDZ. 
 
 Genus—DENTALIUM, Linneus, 1740. 
 (Syst. Nat., Ed. 2, p. 64.) 
 DENTALIUM WOLLUMBILLENSIS, sp. nov. 
 Dentalium lineatum, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., 2, p. 256 (non. Guéranger),. 
 
 Sp. Char. Shell tubular, rather thin, tapering and slightly curved. (Moore.) 
 
 Obs. Three specimens were observed by Mr. Moore in his Queensland series of 
 fossils. According to Stoliczka,t the name D. lineatum was preoccupied at the time Mr. 
 Moore wrote by Guéranger, whose species appears to be a good one. 1 have, therefore, 
 altered the name of the Australian shell as above. 
 
 Prof. R. Tate refers { Moore’s species to Dentaliwm arcotinum, Forbes, but I have 
 not observed the same amount of curvature inthe Australian shell as exists in the Indian. 
 Our species is also shining and smooth. 
 
 Lee. Wollumbilla (The late Rev. W. B. Clarke); Glanmire Block, seventeen 
 miles south-west of Tambo (Mr. Goffage). 
 
 , * See also p. 39 (Unicardium Mecki). 
 
 + Pal. Indica (Cret. Fauna), 1868, ii., Pts. 7-10, p. 443. 
 t Proc. Austr. Assoc. Adv. Sci. for 1888 [1889], i., p. 230, 
 
484. 
 
 Order—TECHTIBRANCHIATA. 
 Family—TORN A TELLID A. 
 
 Genus—CINULIA, Gray, 1840. 
 (Synop. Brit. Mus., 1840.)* 
 
 CrinutraA Hocusterrert, Moore, sp. 
 Acton Hochstetteri, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 256, t. 10, f. 19. 
 
 Sp. Char. Shell rather small, ovate; whorls five; spire rather elevated, acute ; 
 whorls covered by close, distinct, encircling transverse strie, about thirty in number on 
 the body-whorl, which is rather convex ; aperture not exposed. (Jfoore.) 
 
 Obs. In general appearance this shell is not unlike Acteon pullus, Lycett, but 
 the striz with which it is ornamented are much more numerous. It was named by Mr. 
 Moore in honour of Dr. F. von. Hochstetter, Author of the Geological Narrative of the 
 Voyage of the Austrian Frigate ‘“‘ Novarra.” 
 
 I am indebted to Prof. R. Tate for suggesting the reference of this species to 
 Cinulia rather than Act@on, on account of the thickened outer lip and strong columella 
 fold. 
 
 Loc. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Genus—AOTAION, De Montfort, 1810. 
 (Conch. Systématique, ii., p. 315.) 
 
 Actmon DEpRESsUS, Moore, Pl. 29, fig. 9. 
 
 Actwon depressus, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 256, t. 10, f. 20. 
 
 Sp. Char. Shell small, conical; spire with five volutions, rather depressed ; 
 body-whorl with about fifteen rather distinct strie ; aperture ovate. (Moore.) 
 
 Although this shell is not in good condition, it is clearly separable from Acteon 
 [Oinulia| Hochstettert by its more depressed figure, and by the difference in the 
 external strix. (Moore.) . 
 
 Mr. Hudleston’s figure of Acteon or Avellana, sp.,t from South Australia, is 
 probably a better representation of the present species than either Moore’s illustration 
 
 or that given here. 
 Loc. Wollumbilla (The late Rev. W. B. Clarke) ; North-east end of Glanmire 
 Block, seventeen miles south-west of Tambo (Mr. Goffage). 
 
 Order—SCUTIBRANCHIATA. 
 Family—PLEUROTOMARIIDA. 
 
 Genus—PLEUROTOMARIA, Defrance, 1824. 
 (Tableau Corps Organ. Foss., p. 114.) 
 
 PLEevROoTOMARIA ? Cuirront, Etheridge, Pl. 29, fig. 10. 
 Pleurotomaria Cliftoni, Etheridge, Quart. Journ. Geol. Soc., 1872, xxvili., p. 347, 6. 25, f. 4. 
 Sp. Char. Shell trochiform, spire elevated, apex acute, whorls four to five, 
 rapidly increasing, body-whorl large ; aperture large and nearly round, base convex; 
 columella thick, umbilicus apparently wanting or very small. ( Etheridge.) 
 
 
 
 * Fide Agassiz, Nomen. Zool. (Gen. Moll.), p, 19. 
 + Geol. Mag., 1890, vii. (3), p. 243, t. 9, f. 4. 
 
485 
 
 Obs. The body-whorl is more than double the dimensions of the preceding or 
 fourth whorl, and proportionally much more globose, and crossed diagonally by delicate 
 lines of growth at an angle of 45°. The rather broad sinus occupies the upper 
 half of the body-whorl. I find great difficulty in referring this shell specifically to any 
 known British form. It, however, resembles Turbo (Pleurotomaria) Dunkeri, Goldf., 
 from the Middle Lias. (Htheridge.) 
 
 The resemblance of this species to a typical Plewrotomaria is not a marked one ; 
 in fact, it is very much more like those Paleozoic shells called Mwurchisonia, with 
 rounded whorls. Nor does the word “ trochiform” strictly describe its shape; it might 
 be better described as conically or elongately turbinate. 
 
 Loe. Gordon Downs, near Roma (The late R. Daintree). 
 
 _Family—TROCHID. 
 
 Genus—DELPHINULA, Lamarck, 1804. 
 (Ann. Mus. Hist. Nat. Paris, iv., p. 108.) 
 
 DeELPHINuLA ? REFLECTA, Moore, Pl. 29, fig. 12. 
 Delphinula reflecta, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 256, t. 10, f. 21. 
 
 Sp. Char. Shell rather small, turbinated; whorls 3-4; spire slightly elevated ; 
 volutions separated by an encircling sinus; body-whorl much increased ; aperture 
 circular, with a thick reflected lip. (JZoore.) 
 
 Obs. The present species is either a very aberrant form of Delphinula, or it 
 cannot be referred to that genus, for it is hardly necessary to observe that neither the 
 inner nor the outer lip of Delphinula is reflected, in the proper sense of the word. 
 
 Loe. Wollumbilla (Lhe late Rev. W. B. Clarke). 
 
 Order—PECTINIBRANCHIATA. 
 Family—NATICIDA. 
 
 Genus—NATICA, Adanson, 1757. 
 (Hist. Nat. Sénégal, Coquil., p. 172.) 
 
 Natica VARIABILIS, Moore, Pl. 31, figs. 2 and 3. 
 Natica variabilis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 256, t. 10, f. 15. 
 lineata, Etheridge, Ibid., 1872, xxviii., p. 342, t. 21, f. 1. 
 sp., Hudleston, Geol. Mag., 1884, i., p. 339, t. 11, f. 4. 
 
 Sp. Char. Shell very thick, broader than high ; spire of 3-4 volutions, somewhat 
 depressed ; body-whorl increasing rapidly in size and extended; aperture ovate; 
 umbilicus small. (MMoore.) 
 
 Obs. This species is abundant, and I have had an opportunity of examining 
 specimens in various conditions. When the body of the shell has been worn, it presents 
 a rugosely striated surface; but in smaller examples, in which the shell is usually better 
 preserved, the test is seen to have a comparatively smooth striated exterior. (/oore.) 
 
 It closely resembles NV. gaultina, from the Gault of Folkestone and the Green- 
 sand of Blackdown. 
 
 The suggestion thrown out by Mr. Etheridge, that his species is probably 
 identical with Moore’s previously described one, has been adopted by Prof. R. Tate,* 
 who has united them. It is the same as Mr. Hudleston’s unnamed shell. Natica 
 
 99 
 
 ” 
 
 * Trans. R. Soc. S. Australia, 1885, vii., p. 75 ; Proc. Austr. Assoc. Adv. Sci. for 1888 [1889], i., 
 p. 180, 
 
486 
 
 variabilis appears to have a wide geographical distribution, for it is one of the shells 
 obtained by Mr. Chandler * in the neighbourhood of the Peake, Central Australia. 
 
 Loc. Wollumbilla (The late Rev. W. B. Clarke); Maranoa River, at Mitchell, 
 and Blyth Creek, near Blythsdale Station (G. Sweet—Colln. Sweet, Melbourne). 
 
 Natica ornatisstMa, Moore, Pl. 25, fig. 11. 
 Natica ornatissima, Moore, Quart. Journ. Geol. Soc., 1870, p. 257, t. 10, f. 16. 
 Sp. Char. Shell small, spire depressed ; whorls convex, the last very rounded and 
 globose ; aperture large and circular. (Joore.) 
 Shell-structure smooth, with broad bands of growth at intervals, within or on the 
 surface of which are finer striations. The shell still retains some of its original colour. 
 
 (Moore.) 
 Loc. Wollumbilla (The late Rev. W. B. Clarke). 
 
 Natica Jackit, sp. nov., Pl. 21, fig. 22. 
 
 Sp. Char. Shell ovate, sub-globose, of about four whorls; spire short; upper 
 volutions very short, convex, separated by a moderately marked suture; mouth ovate, 
 nearly straight along the inner lip; the latter is but little reflected or thickened ; 
 umbilicus moderately large; surface of the body-whorl bearing strong, sub-imbricating, 
 oblique, transverse ruge (which are aiso faintly perceptible on the penultimate whorl), 
 crossed on the lower portion of the whorl by oppositely directed, oblique, semi-spiral 
 ruge of different lengths, wider apart than the transverse ridges, and to some extent 
 effacing them, and producing a more or less V-shaped ornament. 
 
 Obs. This peculiar and handsomely seulptured little shell may perhaps be 
 referable to Vanikoro (Narica, Recluz), or even Vanikoropsis, Meek, but I am not yet 
 satisfied how far the sculpture is persistent. The spiral lines start from the inner lip, 
 passing obliquely round the whorl to the outer lip, but during their course are faulted 
 downwards, as the width of the whorl increases. 
 
 I have been unable to find any described species of Natica bearing similar 
 sculpture, even with the assistance of my former Colleague, Mr. Edgar A. Smith. A 
 recent form, Natica cancellata, Lamk., from the Isle of Nevis, is wholly cancellated, and 
 so is a fossil Meritina, described by D’Orbigny,t from the Cretaceous rocks. of South 
 America, in which the spiral strie are confined to a zone all round the body-whorl. The 
 absence of a callosity on the inner lip, irrespective of other features, separates Watica 
 Jackii from both the foregoing. 
 
 In this species the inner lip can hardly be said to be reflected, and there existed a 
 well-marked and elongated umbilical opening. 
 
 Loc. Cloncurry Road, at Julia Creek (R. L. Jack). 
 
 Family—STROMBID &. 
 
 Genus—ANCHURA, Conrad, 1860. 
 (Journ. Acad. Nat. Sci. Philadel., 1860, iv., p. 284.) 
 
 AncHvurRA ? WILKINSONI, sp. nov., Pl. 81, figs. 4 and 5. 
 (Compare Alaria or Anchura, sp., Hudleston, Geol. Mag., 1890, vii. (3), p. 242, t. 9, f. 2.) 
 Sp. Char. Shell (without the expanded lip) fusiform, of six or more whorls, 
 angulated in the middle line, the last unequally biangular; last whorl abruptly con- 
 tracted into the base of the beak below; aperture (?) rhombic oval; the median angular 
 
 * Trans. R. Soc. 8, Australia for 1880-81 [1882], iv., p. 149. 
 + VY. divaricata, D’Umont d’Urville’s Voy. Pole Sud. Géologie, 1847, Atlas, t. 7, f. 43 and 44. 
 
487 
 
 line of all but the last whorl occupied by small, semi-separate nodes ; carina of the last 
 whorl without any apparent upward flexure, but below it is a second and finer sub- 
 parallel keel, which diverges somewhat downwards; general surface covered with 
 revolving striz. 
 
 Obs. The outer lip, with its digitation or digitations, is unknown, and the inner 
 lip not preserved. Through the non-preservation of these portions and the canal, it is 
 difficult to accurately determine the genus to which this shell should be referred. It 
 may be either Aporrhais, Anchura, or Drepanochilus ; but from the divergence of the 
 revolving carine on the last whori, and thereby probably indicating two digitations of 
 the outer lip, one of the two former is the most likely. In their present condition our 
 specimens are not unlike Dicroloma, Gabb.; but the species may for the present be 
 referred to Anchwra provisionally. 
 
 It is possible that the “ Alaria or Anchura” figured * by Mr. Hudleston from 
 South Australia is a different species from A. ? Wilkinsoni. The latter is named in 
 honour of the late Mr. C. S. Wilkinson, Government Geologist of New South Wales. 
 
 Loc. Evora Station, twenty-five miles north-east of Blackall (Rowland Morrisby). 
 
 Class—CEPHALOPODA. 
 
 Order—DIBRANCHIATA. 
 Family—LOLIGINID &. 
 
 Genus—THUTHIS, Schneider, 1784. 
 (Sammlung verm. Abhandl., p. 113.) 
 Obs. Small portions of the shaft of a pen (Pl. 35, fig. 21), with the lateral 
 
 expansion of the wings, indicate the presence of a Cephalopod allied to the Calamarics. 
 The remains are all fragmentary. (Joore.) 
 
 Loe. Wollumbilla (The late Rev. W. B. Clarke). 
 
 Family—BELEMNITID 2. 
 
 Genus—BELEMNITES (G4. Agricola), D’ Orbigny, 1840. 
 (Pal. Frang. Terr. Crét., 1840, 1., p. 37.) 
 
 BELEMNITES AUSTRALIS, Phillips, Pl. 35, figs. 1 and 2. 
 Belemnites australis, Phillips in Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 258, t. 16, f. 1 and 2. 
 
 Sp. Char. Guard hastate, depressed in the postalveolar region by lateral expan- 
 sion ; ventral face somewhat flattened, but without trace of a ventral groove; two lateral 
 grooves sharply cut, and approximating to the ventral face in the alveolar region, thence 
 bending toward the dorsal aspect, and continued in a fine stria on the middle of the side. 
 Length four and a-half inches to the point where the guard grows, thin over the phrag- 
 macone; diameters at the alveolar apex 0°725 and 0°600, further back in the more 
 flattened part 0°770 and 0°600. Avis of the guard 3300. Proportion of axis to ventro- 
 dorsal diameter as 550 to 100, of ventral to dorsal radius as 40 to 60. Phragmacone 
 unknown, its angle 20°. (Phillips.) 
 
 Obs. A much older specimen is a split half, the fissure being dorso-ventral. It 
 shows the lateral groove, marked with a double stria, and the nearly straight-sided 
 excentric alveolus. The axis of the guard is curved, and channelled, as in some specimens 
 
 * Geol, Mag., 1890, vii. (3), p. 242, t. 9, f. 2. 
 
488 
 
 from the Oxford Oolite. The ventral portion is to the dorsal as 40 to 60; the axis, as 
 is usual in old specimens of hastate Belemnites, is not longer than in ae and its 
 proportion to the diameter is reduced to 240 : 100. 
 
 These fossils appear, on the whole, most allied to Belemnites hastatus, Blainville, 
 and to the depressed variety of it which occurs in the Oxford Clay of England. But 
 they are entirely distinct by the lateral grooves being so sharply cut over the alveolar 
 and postalveolar region, and by the absence of a ventral groove. 
 
 There is, indeed, one specimen (the posterior part of a large guard) marked 
 “Upper Maranoa River,” which, with portions of the lateral grooves, shows along the 
 ventral face a partially impressed but interrupted groove, not unlike some appearances 
 of Belemnites sulcatus of the Oxford Clay of England. The lateral grooves show 
 ramifications, and appear not to bend backward. It may be a different but allied species. 
 (Phillips in Moore.) 
 
 The Belemnites described * by Sir James Hector as B, australis, Phill., do not 
 appear to belong to this species at all. 
 
 Loc. Wollumbilla and Upper Maranoa River (Zhe late Rev. W. B. Clarke). 
 
 BELEMNITES Oxys, Ten. Woods. 
 
 Belemnites oxys, Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. 3, p. 237, t. 18, f. 1-3. 
 a australis, Ten. Woods (non Phillips), Joc. cit., p. 286. 
 
 Sp. Char. Guard hastate, with a rather long, very slightly undulating outline, 
 ventral face flattened but without a trace of a ventral groove; two lateral grooves 
 sharply cut, and approximating to the ventral face in the alveolar region, thence bending 
 towards the dorsal aspect with a scarcely perceptible curve and continued in a fine stria 
 on the ventral margin. Length of preserved portion one hundred and forty-five milli- 
 metres, width of the alveolar end twenty millimetres, greatest width at the end of the 
 lateral groove, and about the centre of the fossil twenty-two millimetres, ventro-dorsal 
 width greatest at the broken end, and gradually tapering thence to the point. (Zen. 
 Woods.) 
 
 Obs. B. oxys differs from B. australis in its greater length, tapering outline, 
 and different curvature of the lateral groove. Notwithstanding that it otherwise 
 generally resembles the latter, the outline of the two species is so markedly different 
 as to necessitate their separation, at any rate pending the discovery of intermediate forms. 
 
 Loc. Mount Stewart Run, Grey Ranges, New South Wales, near the South 
 Australian and Queensland borders: 
 
 BELEMNITES EREMOS, Tate, Pl. 35, fig. 6. 
 
 Belemnites paxillosus (Schlotheim), Phillips, Quart. Journ. Geol. Soc., 1870, xxvi., p. 240, t. 16, f. 6a and b. 
 ms eremos, Tate (ms.), Proc. Austr. Assoc. Adv. Sci. for 1888 [1889], i., p. 229. 
 
 Obs. Up to a comparatively recent date the only evidence of this Belemnite as 
 an Australian species was the following quotation from Mr. Moore’s Memoir. He 
 states that two imperfect specimens were obtained from a Wollumbilla block and 
 submitted to the late Prof. John Phillips, who stated that “they belong to young 
 Belemnites and show the phragmacone in situ, and the straight nearly central axis of 
 the guard with a small canal. The cross-section of the phragmacone is distinctly 
 elliptical and oblong ; the siphuncle is clearly enclosed ; longitudinal dorsal strize very 
 distinct. I have made a sketch of these points, which on the whole make me adhere to 
 the opinion of the Oolitic, and perhaps Liassic, affinity of this shell. It appears to be 
 most nearly allied to B. pawillosus, but to be distinct by its elliptical phragmacone ; 
 this ellipticity diminishes with age.” 
 
 
 
 * Trans. N. Zealand Inst., 1878, x., p. 487, t. 28, f. a-e. 
 
 
 
489 
 
 More recently, however, Prof. R. Tate has proposed* for this Belemnite the 
 above name, and believes that the oblique lateral furrows, and the absence of apical 
 furrows, place it near B. australis, Phill. 
 
 Loe. Wollumbilla (The late Rev. W. B. Clarke). 
 
 BELEMNITES SELLHEIMI, Ten. Woods, Pl. 35, figs. 10 and 11. 
 Belemnites Seliheimi, Ten. Woods, Journ. R. Soc. N. S. Wales for 1882 [1883], xvi., p. 150, t. 7, f. 1. 
 
 Sp. Char. Phragmacone extending at an angle of 17°, circular, broken at each 
 end; 100 mm. long, 45 mm. at broad end, and 15 mm. at narrow end; chambers twenty- 
 five in number, slightly oblique, advancing a little on the dorsal face, and retiring on the 
 ventral, with slight lateral flexure ; an obscure carina on the dorsal face, with a distinct 
 shallow groove for the whole length. (Zen. Woods.) 
 
 Obs. Although a portion of a phragmacone is hardly the material on which to 
 establish a species, this name will suffice to distinguish that part of an undoubtedly 
 large Belemnite which occurs in the “ Rolling Downs Formation.” 
 
 It is very probable, as stated by Mr. Woods, that B. Sellheimi corresponds to a 
 large phragmacone of doubtful affinity described by Prof. Phillips, from Wollumbilla,+ 
 
 -and may be identical with it. He says—‘‘ Phragmacone 5°5 inches long, its greatest 
 diameter 1°75, the section nearly circular. Above forty septa can be counted; and the 
 whole number must have been fifty, without reaching the last chamber. The septa are 
 a little oblique, advancing in the dorsal and retiring a little on the ventral face, with a 
 slight lateral flexure. Depth of the chambers about one-sixth of the diameter. 
 Siphuncle clearly internal, its section rather elliptical. The phragmacone is nearly 
 straight, with an angle of 18°.” 
 
 Many years ago the late Rev. W. B. Clarke { named a Belemnite from the same 
 locality as B. Barklyi, but all that is known of this is a remark by Prof. F. McCoy,§ 
 “A large species . . . . nearly related to the gigantic species of the Lower Oolite 
 and Lias of Europe, but which cannot be fully characterised from the present specimen, 
 as all the posterior portion of the guard is broken away.” Possibly thismay be Mr. 
 Wood’s species also. 
 
 My Colleague’s Collection contains a portion of a phragmacone consisting of five 
 chambers, not far removed from the proximal end, one and a-quarter inches in diameter, 
 and each about three-eighths of an inch deep (PI. 35, figs. 10 and 11). The length is 
 one inch, and the siphon small and quite internal. The fragment, so far as preserved, 
 is rather straight-walled, with an ill-defined dorsal carina and a faint groove. The 
 septa advance on the dorsal side and retreat on the ventral, and laterally have a slight 
 flexure. In a great measure agrees with Phillips’ phragmacone above described, but is 
 still more in accord with Woods’ B. Seliheimi. | 
 
 In the Queensland Museum is astill more perfect phragmacone five inches in 
 length with a proximal diameter of two inches, and a distal of three-quarters of an inch 
 without having attained the terminal chamber. There are portions of about twenty-six 
 chambers preserved. 
 
 Loc. Palmer River (P. F. Sellheim) ; Wollumbilla (Phe late Rev. W. B. Clarke) ; 
 Flinders River, near Hughenden (Rev. T. W. Ramm); Walsh River (C. W. De Vis— 
 Queensland Museum, Brisbane). 
 
 * Proc. Austr. Assoc. Adv. Sci. for 1888 [1889], i, p. 229. 
 + Quart. Journ, Geol. Soc., 1870, xxvi., p. 258, 
 
  Ibid., 1862, xviii., p. 246. 
 
 § Trans. R. Soc. Vict., 1865, vi., p. 43. 
 
490 
 BELEMNITES CanHAMI, Tate. 
 
 Pl. 35, figs. 3-5, 7-9, 12-14; P Pl. 39, figs. 6 and 7. 
 
 Belemnitella diptycha, McCoy (ms.), Ann. and Mag. Nat. Hist., 1867, xix., p. 356; Ibid., 1867, xx., p. 196. 
 » rans. R. Soc. Vict., 1868, tere i, p. 42. 
 Beloit Cendiams Date. Prot R. Soc. 8. Austr. for 1879- 80 [1880], p. 104, t. 4, f. 2a-2c. 
 
 Sp. Char. Guard hastate terminating in an acute sub-mucronate, central point, 
 contracted in the medio-alveolar region, compressed ventro-dorsally, the ratio of the two 
 diameters measured at a little further back than at the alveolar apex is as two to three. 
 Each dorso-lateral face presents, through the whole length of the alveolar region, a deep 
 and sharply cut furrow; in the region of the alveolar apex itmakes an abrupt turn on to the 
 medial line of the side of the guard, then splits into two shallow grooves, separated by a 
 uniform distance about equal to their own width, which are continued to the apex. 
 Phragmacone sub-oblong in its transverse section ; ihe dorso-ventral diameter is to the 
 other in the proportion iat eleven to thirteen ; “plone” sub-internal, and the axis of 
 the phragmocone is nearly straight. Length of the guard four inches; greatest diameter 
 is nine-tenths, and the corresponding shortest diameter is six-tenths of an inch; axis of 
 guard two and a-half inches. (Zuate.) 
 
 Obs. This species differs from B. australis, Phill., “‘in beg more distinctly . 
 
 hastate, much more compressed, and in the lateral grooves being continued into a double 
 sulcus.’ I believe Professor Tate is right in separating from the original figures of 
 B. australis, Phill., two and placing them with the present species. The community of 
 form mentioned by Tate is traceable through several specimens examined by me, notwith- 
 standing the fact that the lateral grooves are not always well preserved. Thus, in 
 Pl. 35, figs. 7 and 8, they are faintly visible, through the surface being much worn, but in 
 fig. 9 of the same piate they are not to be seen at all 
 
 The specimens before me have yielded the following characters :—The guard is 
 sometimes subspathulate or fusiform, but not greatly flattened, almost circular near the 
 distal termination of the alveolar region; thence gradually swelling out, with an elliptical 
 section, and slowly acuminating to the posterior end, which is pointed, or mucronate, 
 but without an extended mucro. The dorso-lateral grooves at their proximal ends are 
 wide and deep, rather far apart, and give to the section quite a pinched-in appearance. 
 The axis of the guard is decidedly excentric, and there seem to be two vascular grooves 
 on each side, but on this point I am not quite satisfiéd. 
 
 For some years now, lists and general notices of Australian Mesozoic fossils, 
 including references of my own, have contained the name of Belemnitella diptycha, 
 McCoy. The meagre remarks made by Sir F. McCoy on this Belemnite make it very 
 difficult to recognise the species; but his comparison with Belemnitella plena, of the 
 European Chalk, renders it much more easy of accomplishment. B. diptycha is said to 
 differ from B. plena by being larger, the dorsal furrows a little farther apart, and the 
 absence of a ventral furrow. I had provisionally named the specimens, Pl. 35, figs. 7-9, 
 Belemnitella diptycha, McCoy, but was always much perplexed by the absence of the ventral 
 groove on which the generic separation between Belemnites and Belemnitella is chiefly 
 based. I have recently been favoured by Sir F. McCoy with the specimen on which he 
 based the name, and to my surprise found it to be only a fragment of the distal end of 
 a guard, indistinguishable from 'T'ate’s Belemnites Canhami. Under these circumstances, 
 the one must be considered as a synonym of the other, and taking into consideration the 
 excellent description of Professor Tate, accompanied by a comprehensive figure, we 
 cannot do less than accept his name, in preference to the hardly diagnosed species of 
 
 McCoy. 
 
 
 
491 
 
 Tt cannot be denied that in general appearance Belemnites Oanhami greatly 
 resembles Belemnitelia plena, especially those figures given by D’Orbigny under the 
 name of Belemnitella vera,* but, of course, so far as we know them, the difference is a 
 generic one. 
 
 Loc. Cambridge Downs Run, Flinders River, six miles from Richmond Downs 
 Station (Mr. Sanders); Aramac Well, at two hundred and thirty-eight feet (S. Shar- 
 wood) ; Flinders River, near Hughenden (Rev. T. W. Ramm); Thurloo [? Thurles], two 
 hundred miles north-west of Bowen, at four hundred feet deep (Dr. J. C. Cox—Mining 
 and Geol. Mus., Sydney); Barcaldine (Vhe late James Smith) ; Wood-duck Creek, near 
 the Peake, Central Australia (Messrs. J. Canham and Chandler, fide Tate—Colln. Tate) ; 
 Base of Walker’s Table Mountain, Flinders River, as Belemnitella diptycha, McCoy 
 (Messrs. Carson and Sutherland, fide McCoy—Colln. National Museum, Melbourne). 
 
 BELEMNITES? LIVERSIDGEI, sp. nov., Pl. 35, figs. 17-20. 
 
 Sp. Char. Guard small, elongate, claviform, posteriorly extended or graduated into 
 a mucro of greater or less length, depressed (from dorsal to ventral) but not compressed 
 (from side to side), from three-quarters to one and a-half inches long; ventral surface 
 bearing a groove extending for about half the guard length, and sometimes even more ; 
 axis very excentric and ventral, superficial, and shown on the surface as a light-coloured 
 line; section oval to elliptical; lateral vascular markings double, very fine, extending 
 the whole length of the guard. 
 
 Obs. I have ventured to describe this peculiar little Belemnite under the above 
 name, believing it to be new to ‘Australia, in honour of Professor Archibald Liversidge, 
 F.R.S , of Sydney University, to whom I am indebted for an opportunity of examining 
 many interesting fossils. 
 
 The shape at once reminds us of B. minimus, Lister, of the Gault, by the 
 extended pipe-like posterior end, and the size. It is distinguished, however, by the 
 marked excentricity of the axis of the guard, which in our species is only superficial. 
 There appears to be a long ventral groove, but how far this extends it is difficult to say, 
 as the proximity of the axis to the surface seems to have produced a line of least 
 resistance, and sometimes gives rise to a crack. 
 
 In one example (Pl. 35, fig. 18), which may be this species, is a fine grooved 
 line on the guard, also impressed on the phragmacone, which is partially preserved, - 
 passing through all its shelly layers. Viewed from this light, the crack above mentioned 
 is probably in place, and represents the ventral groove, which extends the whole length 
 of the guard. 
 
 The excentricity of the axis is well shown in some cross-sections, and in such it 
 is seen to approach the periphery immediately below the outermost shelly layer. 
 
 Pl. 35, figs. 17, 19, and 20, seem to show a central canal along the axis line of the 
 guard, which is made apparently by weathering. This may be related to an extension 
 of the initial spherule, as described by the late Prof. J. Phillips, who says—“ It is 
 supposed by some writers to have been extended backward into a small canal at the 
 meeting of the fibres along the axis of the guard,’ &c. The latter is very apparent in 
 some of our specimens, and it is equally clear that it becomes a canal or tube. Fig. 19 
 may be explained in this way, or perhaps it may be a portion of the alveolus with the 
 siphon remaining. 
 
 Hauer has described a species from New Zealand under the name of B. auck- 
 landiensis,t which to some extent resembles our species. 
 
 
 
 * Pal. Frang. Ter. Creét. Ceph. i,, Suppl., 1847, t. 2. 
 + Reise Osterr. Fregatte Novara, 1857-59, Geol. Theil., Bd. i., 2 Abth., 1865, p, 29, t. 8, f. 3c. 
 
492 
 
 These little Belemnites have also some resemblance to B. hastatus, Blainville, from 
 the Oxford Clay; but the anterior end of our form, as in B. minimus, is much too 
 short, and the ventral groove in no way corresponds to the depth and distinctness of the 
 former. It is also quite distinct from B. pistiliformis, Blainville, being distinguished 
 by its posterior mucro. 
 
 Loc. Aramac (The late James Smith). 
 
 BELEMNITES, sps. 
 
 Obs. Inaddition to the species described, sundry interesting fragments have 
 from time to time come to light. Mr. R. Etheridge, F.R.S., referred * to phragmacones 
 and alveolar cavities from Beleombe Creek, Black Downs, and compared them to 
 B. abbreviatus of the Oxford Clay and Coral Rag. 
 
 The late Prof. J. Phillips referred to a small species from the Upper Maranoa in 
 the following words+ : ~“‘ Here is a small nearly cylindrical Belemnite, with a sub-central 
 axis and an acute-angled alveolar cavity. It has one long narrow groove, not clearly 
 seen to be a ventral groove. Though incompletely exhibited, it must be a distinct 
 species from the others. . . . . It is not one of the Canaliculati, but more probably 
 one of the Hastati.” 
 
 From Blackall Road, nine miles from Tambo, my Colleague has collected several 
 fragments, two of which are figured. In Pl. 35, fig. 15, is seen a phragmacone and 
 portion of a guard. The former is one and a-quarter inches long, and possesses from 
 sixteen to eighteen chambers. The entire specimen is three and three-quarter 
 inches long. 
 
 The specimen illustrated in Pl. 35, fig. 16, differs from the preceding figure in the 
 larger number of chambers in the phragmacone, and in their lesser depth. There are 
 twenty-three or twenty-four chambers in the space of one inch. 
 
 Order—TETRABRANCHIATA. 
 Family—AMMONITID &. 
 Genus—AMMONITES, Auctorum. 
 Section —AMALTHEUS. 
 
 AMMONITES OLENE, Ten. Woods, Pl. 29, fig. 5; Pl. 80, fig. 4. 
 Ammonites olene, Ten. Woods, Journ. R. Soc. N.S. Wales for 1882 [1883], p. 150, t. 7, f. 2, t. 8, f. 1. 
 
 Sp. Char. Shell much compressed, periphery narrowed to an acute angle; 
 whorls eight and a-half probably; umbilicus apparently narrow; sutures very 
 indistinct, apparently seven, much divided, rounded lobes on each side; diameter, 
 103 mm., thickness 17 mm.; surface crossed by rather broad obtuse sigmoidal ribs 
 which are rather acutely bent in the middle, some few bifurcate. (Zen. Woods.) 
 
 Obs. This Ammonite is compared by its author to A. biflexousus, D’Orb.,t from 
 the Great Oolite, but the keel is not so acute, otherwise there appears to be but little 
 difference between the two species, so far as outward appearance goes. It also 
 resembles the Cretaceous A. cultratus, D’Orb.,§ but the ribs are much more sigmoidal 
 in the Australian fossil. 
 
 
 
 * Quart. Journ. Geol. Soc., 1872, xxviii., p. 346. 
 + Ibid., 1870, xxvi., p. 259. 
 
 Teeals Eran Terr. Jura, 1842, i., p. 422, t. 147. 
 g Jvid., Terr. Cret., i., p. 145, t. 46, f. 1 and 2, 
 
 € 
 
 
 
 
 
493 
 
 T have seen an Ammonite from Primrose Springs, South Australia, collected by 
 H. Y. L. Brown, very closely allied to, if not identical with, this species.* 
 Loc. Palmer River (The late Rev. J. EH. T. Woods). 
 
 AMMONITES WALSHENSIS, sp. nov., Pl. 42, figs. 10 and 11. 
 
 Sp. Char. Shell discoid, thin, much compressed; whorls high, increasing very 
 rapidly in size, the inner more or less concealed; umbilicus narrow, moderately deep, 
 and small for the size of the shell ; mouth sagittate ; back exceedingly sharp and without 
 a defined keel; flanks almost flat, having the slightest possible convexity, but imme- 
 diately below the knife edge of the back slightly concave, surface with faint geniculate, 
 or partially sigmoidal, delicate riblets, strongest around a line almost midway between 
 the umbilicus and edge of the shell, and there producing a very slightly perceptible 
 ridge; between the riblets at this point area series of wrinkles which assist in producing 
 this median line, and breaking the general continuity of the flanks ; towards the periphery 
 spiral lines are visible, but without causing any marked reticulation; sutural characters 
 unknown. 
 
 Obs. In form this Ammonite resembles many Lower Mesozoic and Cretaceous 
 forms. Its outline closely follows that of Ammonites (Amaltheus) lymensis, Wright,+ 
 but the ornament of the two shells is different. The spiral lines remind us of 
 A, (Amaltheus) margaritatus, Mont.,{ but the cordate keel and large open umbilicus of 
 the latter at once separate the two species. 
 
 Amongst Cretaceous Ammonites, A. complanatus, Mantell, of the Grey Chalk, 
 may be referred to. In form, but not wholly in structure, our species resembles 
 A. clypeiformis, D’Orb.,§ from the Neocomian, but it is more compressed, and the former 
 appears to bea plain shell with a moderately open umbilicus. In the small condition 
 of this feature, and the sharp back, A. walshensis is brought into close contiguity with 
 Ammonites requienianus, D’Orb.,|| which is very similar to the present species except 
 for its closed and very small umbilicus. 
 
 Referring again to A. complanatus, Mantell,{| notwithstanding the great similarity 
 -inshape to A. walshensis, including even the wrinkled median line on the flanks, there 
 appears to be an absence of the spiral lines, and with these is the remarkable peculiarity 
 of a pin’s-point umbilicus, and a flat narrow back. 
 
 My friend, Dr. Henry Woodward, to whom a photograph of this Ammonite was 
 sent, suggests a comparison with Ammonites D’ Orbig gnyanus, Geinitz, but a figure of 
 this pret is not accessible to me. 
 
 Loc. Walsh River (Hann’s Expedition—Queensland Mus.**) 
 
 Section—SCHL@NBACHIA. 
 AMMONITES INFLATUS, J. Sowerby, var., Pl. 34, figs. 1-4. 
 Ammonites inflatus, J. Sowerby, Min. Con., 1817, ii., p. 170, t. 175. . 
 
 A) 7 D’Orbigny, Pal. Franc. Terr. Cret., 1840, i., p. 304, t. 90. 
 Bs x Stoliczka, Pal. Ind. (Cret. Ceph.), Ser. 3, 1861, Pt. i, p. 48, tt. 27, 28, 29, and 30, 
 feoless 
 
 Sp. Char. Shell discoid, sub-compressed, not greatly inflated, strongly carinate, 
 four or five whorls visible, ovately quadrangular in section; umbilical cavity freely 
 
 
 
 * This has lately been described by Mr. W. H. Hudleston as A. fontinalis (Geol. Mag., 1890, 
 vii. (3), p. 241, t. 9, f. 1). 
 
 + Mon. Lias. Ammonites, 1881, Pt. 4, t. 48, f. 1 and 2. 
 
 + Ibid., 1882, Pt. 5, t. 53. 
 
 § Pal. Frang. Terr. Cret., i., p. 187, t. 42, f. 1 and 2. 
 
 \| Tbid., p. 93. 
 
 ‘I See Sharpe, Mon. Chalk Moll., Pt. i., 1853, t. 7, f. la and b. 
 
 ** Therefore probably collected by Mr. Norman Taylor, Geologist to the Expedition. 
 
494. 
 
 exposing the embraced whorls; ventral surface (or back) obtusely rounded; keel 
 prominent, erect, and rounded. In the septa the siphonal lobe is short and broad, 
 almost plain-margined; ventral lobe rather deep; ventral saddle broad, of two chief 
 portions, deeply divided at their sides, each being again subdivided at their apices ; 
 superior lateral lobe deep, and unequally subdivided, being tripartite ; first lateral saddle 
 short and bifureate; inferior lateral lobe short, with two lateral and two terminal 
 divisions; second lateral saddle resembling the first; the whole occupying about three 
 and a-quarter ribs, pectinations strong. The transverse ornamenting coste are 
 tuberculated, frequently bifureating, the division in each case taking place clear of the 
 umbilical cavity ; the largest tubercles are along the sides of the back, and are them- 
 selves transversely crenulated, whilst those around the umbilical edge are also very 
 prominent; on the embraced whorls a single row of tubercles is visible, the intercostal 
 surfaces aré finely transversely striate. 
 
 Obs. A careful comparison with authenticated specimens of Ammonites inflatus 
 leaves little doubt that we have in the Queensland fossils a variety very closely 
 assimilating to the parent species ; the only difference I am able to point out lies in the 
 possession of a rather narrower back, the space between being more acute than in the 
 type form. So much variation occurs amongst Neocomian Ammonites, especially as 
 regards age and locality, that the foregoing points, other characters being equal, can 
 hardly debar the Queensland shells from being placed in this species. This variation in 
 the keel gives to the general outline a more acutely quadrangular shape. The form 
 otherwise, ornament, and general features are particularly alike in the fossils of the 
 two hemispheres, but the figures given by the late Dr. Stoliczka of 4. inflatus from the 
 Indian Ootatoor Group, even bear closer resemblance to the Australian variety than do 
 those of the species proper from Europe. 
 
 A fragment of an Ammonite (PI. 34, fig. 4), collected at Aramac by the late Mr. 
 James Smith, is also probably referable to Ammonites inflatus, as there are traces of 
 strong tuberculated costez, and tubercles around the umbilical edge. 
 
 It is again possible that a small Ammonite represented in Pl. 42, fig. 12, may 
 be this species, although the cost are more sigmoidally bent. This is an impression on 
 the fractured end-surface of a bore-core, and the impression is one inch in diameter. 
 The whorls are few, and there is a forward prolongation of the ventral edge into a well- 
 marked rostrum. The flanks bear coarse, strong, sigmoidal ridges, with here and there 
 smaller interpolations. The form of the back is unknown. In addition to a general 
 resemblance to A. inflatus, this little Ammonite recalls to mind such forms as A. denarius, 
 Sby., A. dautus, Parkinson, and other Cretaceous species. 
 
 Loc. North-east end of Glanmire Block, seventeen miles south-west of Tambo 
 (Ilr. Goffage) ; Aramac, Pl. 34, fig. 4 (The late James Smith); Warriana Bore, 
 at a depth of three hundred and seventy-five feet, twenty-eight miles from Hughenden, 
 on the Winton Road (J. B. Henderson). 
 
 » 
 Section—HAPLOCERAS. 
 
 AMMoNITES FuinpERstI, MeCoy, Pl. 30, figs. 1-3. 
 
 Ammonites Flindersi, McCoy, Ann. and Mag. Nat. Hist., 1865, xvi., p. 334; Jbid., 1867, xx., p. 196. 
 Rs cs McCoy, Trans. R. Soc. Vict., 1866, vii., p. 51; Zbid., 1868, viii., Pt. 1, p. 42. 
 7 Beudanti, var. Mitchelli, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 345, t. 23. 
 3 Flindersi, Etheridge fil., Cat. Australian Foss., 1878, p. 115. 
 Sp. Char. Shell discoidal, compressed, composed of four or five whorls rapidly 
 increasing and about one-fourth of the width of each exposed in an obtusely angular- 
 edged, flat-sided umbilicus ; periphery narrow, sides nearly flat, ornamented with gently 
 
 
 
 
 
 
 
495 
 
 elevated undulating or sigmoidal ribs or folds bending towards the aperture, and about 
 half an inch apart on the middle of the whorl. These and the interspaces are occupied 
 by delicately arranged equidistant parallel lines or coste, which pass over the back; 
 aperture oval, back rounded and narrow, no keel; inner whorls exposed; walls of 
 umbilical cavityangular, flat-sided, or bevelled and smooth; seven much-divided lobes in 
 the septa of each side, two of which are within the edge of the umbilicus. (McCoy and 
 Etheridge.) 
 
 Obs. This Ammonite, inits intermittent folds, involution of whorls, and general 
 habit, much resembles A. Beudanti, D’Orb., from the Gault of England and France, to 
 which it is certainly closely allied. This is the opinion of Mr. R. Etheridge, F.R.S.; and 
 Sir F. McCoy’s appears to have been the same, for he says: “So nearly identical with 
 the very common A, Beudanti (Br.) of the French Lower Chalk, that, but for being 
 slightly less compressed, anda slight difference in some of the septal lobes, it could 
 scarcely be separated, even as a variety.” 
 
 I have examined the type in the National Museum, Melbourne, and believe Mr. 
 Etheridge’s var. Mitchelli to be a synonym of Sir F. MeCoy’s species. 
 
 A very small and neat, smooth and discoidal Ammonite (Pl. 30, figs. 5 and 6), 
 with nearly flat sides, has been found in the mud-stone of Aramac Well. ‘The shell is 
 flat, of three to four whorls, umbilicus small, the back semi-rounded, with a very delicate 
 keel, and a thin test. With the exception of the keel this appears very like what the 
 young of A. Flindersi would be. It is of the same character and proportions, butis even 
 more like that of A. Gardeni, Baily,* which has similar whorls and keel. The latter is 
 common to the Cretaceous of both South Africa and India. 
 
 The back of the little Ammonite is too broad for A. olene, Woods, and there are 
 no transverse ruge, although they are, to some extent, of the same type. 
 
 Loc. Base of Walker’s Table Mountain, Flinders River (Messrs. Sutherland 
 and Carson—National Museum, Melbourne); Hughenden Station, Flinders River (Zhe 
 late R. Daintree ; G. Sweet—Colln. Sweet, Melbourne) ; [? Barcaldine Railway Station, 
 Central Railway (R. Sexton); ? Aramaec Well, at two hundred and ninety feet 
 (S. Sharwood)}. 
 
 Ammonites DaintreEEI, ELtheridge, Pl. 29, figs. 1-3. 
 Ammonites Daintreei, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 346, t. 24. 
 
 Sp. Char. Shell discoidal; whorls depressed or flattened at the sides, with a 
 rather narrow rounded back. The sides of the shell ornamented with numerous nearly 
 equal and closely arranged ribs, all of which are slightly arcuated, and pass over the 
 back or dorsal edge; umbilicus wide and deep, allowing half the inner whorls to be 
 exposed ; sides of the whorls around the umbilicus steep-sided, rounded, or subangular ; 
 aperture broadly oval, the outer whorl embracing two-thirds of the next inner whorl. 
 The ribs at the terminal portion of the last or body-chamber are somewhat unequal and 
 coarser. 
 
 Obs. I have searched every available source for information relative to this 
 shell, and cannot recognise any species approaching it in the Cretaceous rocks of 
 Europe, India, or America. It has some affinity with A. astertanus, D’Orb., but wants 
 the tubercle around the umbilicus; and the ribs are greatly bent or slightly sigmoidal, 
 whereas in A. asterianus they are straight. It also resembles, in the ribs, some forms 
 or varieties of A. Herveyi, but is not so tumid a shell. It occurs associated with 
 A. Beudanti, D’Orb., Ancyloceras and Inoceranmi, in the Hughenden Beds. (Htheridge.) 
 
 Loc. Wughenden (The late R. Daintree; G. Sweet—Colln. Sweet, Melbourne). 
 
 
 
 * Quart. Journ. Geol. Soc, 1855, xi., t. 11, f, 8a and 6. 
 
496 
 
 Ammonites SurHERLANDI, Etheridge, Pl. 29, fig. 6. 
 Ammonites Sutherlandi, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 345, t. 21, f. 4. 
 
 Sp. Char. Shell discoidal; whorls three or four, with flattened sides and six 
 or seven transverse wavy furrows on the outer whorl; these are slightly inflected 
 forwards on the sides of the shell, and pass over the back at right angles to the keel; 
 back sharply convex; the surface of the shell appears to have been marked by, or 
 ornamented with, fine lines or strie apparently arranged at a different angle from the 
 sulci or furrows. Umbilicus small, well exposed, its walls rounded; aperture oval, 
 elongated, or acutely ovate. (theridge.) 
 
 Obs. Averysmall portion only of the shell remains upon the side of the outer whorl, 
 between the last two sulci, and shows faintly the fine undulating lines. The sutures 
 are so indistinctly marked that the shell cannot be referred to any known species. 
 
 A, Sutherlandi has affinity with A. cassida, Raspail, from the Neocomian,* but the 
 sulci or furrows are fewer and wider, and the umbilicus smaller. None of the group 
 Ligati, in the fine Indian Collection named and described by Ferd. Stoliezka, affords any 
 clue to the form from Queensland, although some twenty-eight Indian species belong to 
 this group. The smallness of the umbilical cavity and depth of the outer whorl remove 
 this form from any species with which we can ally or compare it. (Htheridge.) 
 
 Loe. Marathon Station (The late R. Daintree; G. Sweet—Colln. Sweet, 
 Melbourne). 
 
 AMMONITES SUTHERLANDI, McCoy, MS. 
 Ammonites Sutherlandi, McCoy, Trans. R. Soc. Vict., 1868, viii., Pt. 1, p. 42. 
 
 Obs. The only information we have regarding this Ammonite is the following 
 passage by Prof. Sir F. McCoy :—‘ A new.small species like the French A. Paran- 
 diert,t of the Gault.” Sir F.McCoy’s name, although having precedence over that 
 given by Mr. R. Etheridge, F.R.S., in point of time, cannot retain its position, 
 simply from the want of adequate description, and is, in fact, merely a manuscript name. 
 It is just possible that both Authors have had the same species before them. Prof. 
 McCoy compared his shell to Ammonites Parandieri, to which Mr. Etheridge’s figure 
 also bears considerable resemblance. Both the latter shells have similar wavy furrows, 
 but in Mr. Etheridge’s species the umbilicus is very much more concealed. As both 
 shells, should they prove distinct, cannot retain the same name, a new one for MeCoy’s 
 MS. A. Sutherlandi, will be required. It is to be regretted that material is not forth- 
 coming for a full and proper description. 
 
 Loe. Base of Walker’s Table Mountain, Flinders River (Messrs. Sutherland 
 and Carson—National Museum, Melbourne). 
 
 Genus—HAMITES, Parkinson, 1811. 
 (Org. Remains, iii., p. 144.) 
 
 HAMITES P LAQUEUS, sp. nov., Pl. 42, figs. 14 and 15. 
 
 Sp. Char. Shell oval, link-shaped, but the two extremities free, no helix ‘or 
 involute portion ; section at the older or proximal end nearly round, but compressed and 
 oval at the younger or distal extremity. Surface of the older portion with close, 
 encircling, usually simple, but occasionally bifurcating coste, which gradually broaden 
 out as the shell expands, and become sharp and erect with wide intervals or valleys ; 
 cost on the dorsal side horizontal or very slightly concave, and nearly horizontal on the 
 
 
 
 * Lycée, p. 115, No. 2; Ann. Sci. d’Observation, t. iii., Pl.-11, f. 3. 
 + D’Orbigny Pal. Frang. Terr. Cret., i., pp. 129 and 276, t. 38, f. 7-9. 
 
497 
 
 ventral side, slightly sigmoidally curved on the flanks ; tubercles occasionally developed 
 on the older ribs, a line bordering the siphuncle on each side, and one, or sometimes two, 
 on each flank ; siphuncle small ; chambers about two and a-half lines thick. 
 
 Obs. This peculiar shell is provisionally referred to Hamites, and is only known 
 to me in the semi-convolute link-like form figured. The above description, therefore, 
 only applies to specimens in such a condition. In an ordinary Hamites the two 
 extremities are returned and approach one another in the same plane, the small or older 
 end being again recurved on itself. The returning is so arranged that the growth of 
 the individual could go on uninterruptedly from the one extremity without interfering 
 with that of the other. In the present shell, however, the curvature is such that the 
 extremities, being in the same plane, approach one another, so that in its present state of 
 preservation a disunited link is formed. The first example of this I took to be either a 
 malformation or one in which fracture had displaced one or other of the ends. Butas 
 there is no trace of misplacement, and as other individuals are exactly similar, neither 
 of these hypotheses will hold, and we can only regard it as a particular feature of the 
 species. At the same time, it is manifest that if the younger end continued to grow in 
 the same plane and direction it would ultimately abut against the older and smaller 
 extremity. To what distance the latter extended before the crozier, or initial point, as the 
 case may be, would be reached, it is impossible to say, as all the specimens are broken 
 short off when the two portions approach one another. At the rate of attenuation the 
 proximal end could not have been greatly extended, probably not more than three inches 
 in the largest example.’ 
 
 In the figured specimen the distal or larger end has rather the appearance of a 
 terminal growth, but there is no trace of a definite margin. 
 
 One specimen possesses the proximal end tuberculated, but other examples do 
 not show such ornament. 
 
 It would appear that the present species falls more readily into Hamulina * 
 rather than Hamites. In the former the shell is only once bent upon itself, the parts 
 not in contact, and is without a “ crozier,” but, unfortunately, D’Orbigny is said by 
 Pictet+ to have abandoned his genus and it has probably, therefore, little stability. 
 The curvature of the shell being in one plane renders a comparison with Helicoceras 
 useless. 
 
 Loc. Tower Hill, Landsborough River (The late R. Daintree—Queensland 
 Mus.) ; Warrego River—Queensland Mus.; Wellshot Run, near Barcaldine (4. 
 Lymburner). 
 
 Genus—ANCYLOCBERAS, D’ Orbigny, 1842. 
 (Pal. Frang. Terr. Crét., i., Pt. 2, p. 491.) 
 
 ANCYLOCERAS FrinpErst, McCoy, Pl. 33, fig. 3; Pl. 34, figs. 5-8. 
 
 Ancyloceras Flindersi, McCoy, Ann. and Mag. Nat. Hist., 1867, xix., p. 356, 
 i 5 Etheridge fil., Journ. R. Soc. N. S. Wales, 1883, xvii., p. 89, 2nd pl. (upper fig.) 
 
 Obs. This species has never been described in detail, but Sir F. McCoy says it 
 exceeds the Ancyloceras gigas, Sby., in size, and differs by having the transverse ribs 
 larger and forking on the sides, and the presence of a row of large compressed tubercles 
 on each side of the back. He further considers its nearest ally to be the Ancyloceras 
 Taberelli, Astier, of the French Lower Greensand. The type in the National 
 Museum, Melbourne, to which access was kindly given me by Sir F. McCoy, isa 
 fragment eight inches long, with tubercles along the sides of the back. From each of 
 these two to three ribs arise passing to the flanks. The ribs on the back are double. 
 
 * D’Orbigny, Prod. Pal. Strat., 1852, ii., p. 66. + Traité de Pal., ii., p. 707. 
 2H 
 
498 
 
 In a collection of Australian fossils forwarded to me, when in London, by Prof. 
 Liversidge, I identified what was believed to be a large fragment of this species from 
 Landsborough Creek. I remarked, “Although only a very small portion of the entire shell, 
 it represents an individual of some size, in which the ribs fork on the sides, as described 
 by McCoy, and with a row of large, much compressed tubercles on the sides of the 
 back. The section of our specimen is elliptical, but unfortunately that of A. Flindersi 
 is not given by McCoy.” 
 
 Additional examples of an Ancyloceras, or Crioceras, have been obtained from the 
 strata of Aramac Well in which some of the ribs do fork, as described by McCoy, 
 but not all of them; and there is a clearly marked row of tubercles along each side. 
 The specimens are, therefore, presumed to be A. Flindersi. The following facts are 
 gathered from them :— 
 
 The section was egg-shaped, or elongately pyriform, with flat sides, sloping away 
 rapidly to the narrow back, the dorsal side being broad. The ribs are close in the young 
 state, widening with age, slightly sigmoidal on the flanks, where they bifurcate, each rib 
 on arriving at the edge of the back being enlarged into a tubercle. These, in the young 
 state, are blunt and depressed, but with advanced age becoming more compressed fore 
 and aft. In the older shells also, the ribs become less conspicuous in crossing the 
 flat narrow back. 
 
 The septa are highly complicated, and much broken up. The siphonal saddle is 
 short, whilst the ventral lobes have two chief divisions, or fringes, the outer the longest ; 
 the ventral saddles are quadripartite, having two chief subdivisions, separated by a 
 lobe, consisting of a long terminal, and two lateral fringes; each subdivision is itself 
 split into two smaller saddles, and much pectinated. The superior lateral lobes are 
 very large and long, and occupy as nearly as possible the centre of each flank of the 
 shell, the body of each lobe being long and separated into two large forks, each of 
 which is again, in its turn, slit into two spreading highly pectinated branches. The 
 principal lateral saddle more or less resembles the ventral saddle in its construction ; 
 the inferior lateral lobe is long and narrow, terminating in two chief side branches and 
 a central prolongation; the second lateral saddle is rounded and short, of two divisions 
 separated by a lobe somewhat similar to, but smaller than the lobe subdividing the 
 ventral saddle. 
 
 The chief point in the septal structure of 4. Flinders is the extreme depth and 
 development of the superior lateral lobe and its ramifications. Each lobe occupies a 
 large part of the flank, and in full-grown individuals extends over the width of 
 four ribs. 
 
 Loc. Base of Walker’s Table Mountain, Flinders River (Messrs. Sutherland and 
 Carson—Colln. National Museum, Melbourne) ; Landsborough Creek, Thomson River 
 (Prof. A. Liversidge—Colln. Sydney University); Aramac Well, at two hundred and 
 twenty-four feet, and two hundred and thirty-eight feet respectively (8. Sharwood). 
 
 ANCYLOCERAS TAYLORI, sp. nov., Pl. 42, fig. 13. 
 
 Sp. Char. Shell small, elongate; spire tightly coiled, of about two, or two and 
 a-half whorls ; projected limb gradually increasing in size, not placed precisely at right 
 angles to the spire, but rather obliquely bent towards it; ‘“‘crozier,” or recurved distal 
 end not preserved; coste simple, without tubercles, becoming more obliquely directed 
 as the limb is ascended, rounded, and separated by narrower sulci. 
 
 Obs. The proximal coil of the shell would indicate Ancyloceras rather than 
 Hamites for the reception of this fossil. It may be only the young of some other form, 
 
499 
 
 but if adult is distinct from any,hitherto described Australian species. It is noticeable 
 for the extreme simplicity of its structure, and in this respect would perhaps be 
 included in the group of Ancyloceras pulcherrimus, D’Orb.* 
 
 The name is proposed in honour of my old Friend and former Colleague, Mr. 
 Norman Taylor. 
 
 Loe. Head of the Walsh River + (Colln. Queensland Mus.). 
 
 Genus—CRIOCERAS, Leveillé, 1878. 
 (Mém. Soc. Géol. France, ii., p. 318.) 
 
 CRIOCERAS AUSTRALE, Moore, sp. 
 
 Pl. 30, fig. 7; Pl. 31, fig.1; Pl. 82, figs. 1-4,?5; Pl. 33, fig. 2. 
 Crioceras australe, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 257, t. 15, f. 3. 
 3 », Waagen, Pal. Indica (Jurassic Fauna of Kutch), Cephalopoda, 1875, i., No. 4, p. 246, 
 1. 60, f. 1, a-c. 
 cf Jackii, Etheridge fil., Proc. R. Phys. Soe. Edinb., 1880. 
 ‘A australe, Ten. Woods, Journ. R. Soc. N. S. Wales, 1882, xvi., p. 152, t. 10, f. 5 and 6. 
 S 5 Ratte, Proc. Linn. Soc. N. S. Wales, 1886, i., p. 183, tt. 1 and 2. 
 Compare Crioceras irregulare, Ten. Woods, Jbid., p. 151, t. 8, f. 2.] 
 
 Sp. Char. Shell attaining a very large size, with the whorls massive, broad, close 
 but not touching, from six to eight in number, the first two or two and a-half whorls 
 tuberculate ; back very convex; round or slightly flattened at the sides; dorsal or inner 
 side flat or concave; section roundly deltoid; siphuncle of medium size for that of 
 the shell, immediately below the outer test on the back; septa thick and strongly 
 developed, almost flat in the centre; the ventral or siphonal saddle is short in propor- 
 tion to the inferior lateral saddles. The latter are divided into two strong main 
 branches, each again bifurcating. The second inferior lateral saddles appear to be of 
 equal length with the first, and of similar construction. The ventral lobe is deep, with 
 short branches on each side the dorsal saddle; the digitations are numerous; the coste 
 showing, and very well developed, horizontal on the ventral side or back, slightly 
 sigmoidal on the flanks, and concave forwards on the dorsal side ; simple, or bifurcating, 
 when the latter, consisting of a primary rib, and a subsidiary one at its side, tuberculate, 
 in the young state ; in the latter condition the primary coste are of two sizes, the non- 
 tuberculate ribs being all of one size, whilst those bearing the tubercles are larger, and 
 separated one from the others, sometimes by two and sometimes by three of the former ; 
 coste in the young shell close together, contiguous, but gradually widening out with age 
 and becoming separated by wide rather concave sulci, which become wider still as the 
 mouth is approached ; tubercles blunt and node-like, arranged in six rows, two on each 
 side of the.flank and two on the back, those on the sides becoming less apparent, and 
 disappearing about the end of the second volution ; test striated parallel to the coste. 
 
 Obs. Through a fine series of specimens forwarded to me by Mr. C. De Vis, 
 supplementing additional ones collected by my Colleague, Iam able to trace this species 
 from a comparatively young state (Pl. 30, fig. 7), in which the tubercles are present as 
 little fine nodes, up to the fine specimen figured on Plate 31, of half the natural size; 
 and further, to show that in all probability Moore’s C. australe and C. Jackii (mihi) 
 are identical. 
 
 As originally described, C. Jackii was known either from the inner tuberculated 
 whorls of larger and older specimens, or from young individuals in which the tubercles 
 were very pronounced. In the latter condition the coste are close, sharp, and 
 
 
 
 * Pal. Franc. Terr. Crét., i., t. 121, f. 3. 
 + The head of the Walsh River is in Paleozoic and Plutonic rocks. The locality is probably lower 
 down the Walsh. (R.Z.J.) 
 
500 
 
 moderately straight, but as the shell grew they became rounder, flatter, further apart, 
 abrupt on their front sides, gradually shelving off into the concave sulcus, and sigmoidal 
 in direction on the flanks. In this condition the shell becomes C. australe, Moore. 
 The tubercles are occasionally retained to the fourth whorl before they disappear, but in 
 most examples they are not visible beyond the second or second and a-half whorl, In 
 no less than four specimens there is no sign of tubercles at all, even in the flattened, 
 rounded ribs in advanced age, which gradually become further apart as the mouth is 
 approached, even to the extent of a quarter of aninch. The coste bearing tubercles 
 are always larger and thicker than the non-tuberculate. The number of secondary ribs 
 between those bearing tubercles varies from two to five. Much variation also took place 
 in the contiguity of the whorls, some being inrolled much more closely than others, and 
 frequently the whorls to all appearance look as if touching, but on fracturing the 
 specimens they are all found to be separate. 
 
 Crioceras australe attains to very large dimensions. The subject of Pl. 31, 
 fig. 1, measures twelve and a-quarter inches in one direction by nine and a-half in the 
 other. Another before me is nine inches by seven and a-half, the breadth of the last 
 whorl from the middle of the back to the umbilical edge being three and a-half inches. 
 But in the Australian Museum is a huge specimen described by the late Mr. F. Ratte, 
 consisting of about half the entire shell, showing the following measurements :— 
 
 Ft. in. 
 Diameter ... a a Ras = a we Roy a 
 Circumference of soebstons noe aa rio a8 Joc aoe ee 
 Girth of older portion ... Sr 3e¢: vo «2a QE 
 Distance apart of the coste at a younger end ee Anis a O 4 
 Depth of valleys between the cost# at the younger end a4 go W al 
 
 Mr. G. Sweet obtained another very large example from the Maranoa River, 
 with a diameter of two feet nine inches and even then imperfect. The coste or 
 ribs are from two to three inches apart. 
 
 Mr. Moore states that in his specimen the mouth measured seven and a-half 
 inches in depth by seven in breadth. The dorsal side of each whorl is flattened, with a 
 space in the middle line corresponding to the dorsal lobe, and bounded by two impressed 
 lines. 
 
 One word more about Crioceras Jackii. Moore’s description and figure are quite 
 inadequate for the proper recognition of C. australe, and I believe I should, therefore, 
 have been justified in retaining mine. But it is difficult to believe that two large species 
 could have existed in the same area, so very alike and only known to differ in the young, 
 state. The figure, however, given by Dr. Waagen is probably conclusive, for in this 
 case there are portions of the large outer whorls of C. australe, embracing an inner 
 fragment resembling C. Jackiz. Such conditions are seen in other Oriocert, such for 
 example as C. Hmerici,* a Neocomian species. His statement that when complete the 
 shell attained nearly twice the dimensions of the huge ©. Bowerbanki, of the British 
 Lower Greensand, would appear to be borne out by the size of the shell already 
 referred to as in the Australian Museum. Mr. R. Etheridge, F.R.S., also recognised 
 a large Crioceras in Mr. Daintree’s Collection, measuring little less than twelve or 
 fourteen inches in diameter, which may possibly be this species. 
 
 The subdivisions of the septa have been excellently figured by Mr. Ratte, from 
 the large specimen in the Australian Museum, but from advanced age they are more 
 complicated than those shown in Pl. 82, fig. 4. 
 
 
 
 * Quenstedt, Handb. Petrefactenkunde, 1885, Atlas, t. 45, f, 21, 
 
501 
 
 Loc. Upper Maranoa District (The late Rev. W. B. Clarke) ; Tate River (A. C. 
 Macmillan) ; Walsh River (Hon. A. O. Gregory and Queensland Museum); Palmer 
 River (The late Rev. J. BE. T. Woods) ; Landsborough Creek, Thomson River (Prof. A. 
 Liversidge); Wollumbilla (G. Sweet—Colln. Sweet, Melbourne) ; Maranoa River, about 
 one mile north of Mitchell Bridge (G. Sweet—Colln. Ibid.). 
 
 CRIOCERAS IRREGULARE, Zen. Woods. 
 
 Pl. 33, fig. 1; Pi 42, fig. 163.8 32. fig. ore 
 Crioceras irregulare, Ten. Woods, Journ. R. Soc. N. S. Wales, 1882, xvi., p. 151, t. 8, f. 2. 
 
 Sp. Char. Shell loosely and irregularly coiled; whorls one and a-half, quite 
 free, but the distance irregular, much compressed at the sides; tuberculate in sixteen 
 rows. The first six obsolete, tubercles, three on each side, conical, short, close on the 
 sides, but at an interval on the dorsal edge, then disappearing except that a faint 
 row seen near the end of the fragment after a long interval. Costs of two sizes, 
 the tuberculate ones large, and separated from one another by simple, narrow, round, 
 undulating ribs, which vary in number between the tubercles from two to thirteen. 
 (Len. Woods.) 
 
 Obs. The above description is quoted from the late Rev. Mr. Woods’s Paper 
 word for word, and with identical punctuation. The latter, in the second sentence, 
 seems to have become misplaced, because the sense and meaning of the paragraph does 
 not appear to be continuous. 
 
 The figure of this species certainly represents a more loosely coiled shell than 
 C. australe, but nevertheless the resemblance between the form of the coste and 
 arrangement of the tubercles is so conspicuously alike that a connection between the 
 two cannot but be suspected. The original figure is given in PI. 33, fig. 1, and here 
 will be noticed the apparent tapering termination, or rather commencement, or nucleus, 
 of the shell, this free and open state being quite different to anything yet noticed in 
 ©. australe, the initial portions of which are represented in Pl. 30, fig. 7, and Pl. 32, 
 fig. 1. There are two, three, four, and six coste at times between the larger node- 
 bearing ribs, and these seem to occur irrespective of order (Pl. 33, fig. 1). This is the 
 case in CO. australe, and, as in that species, the nodes cease suddenly, and are-confined to 
 a limited portion of the surface only. Two very prominent nodes occur on the back 
 (Pl. 42, fig. 16), one at each side, immediately below these (Pl. 42, fig. 16), and one or 
 two on each flank (Pl. 33, fig. 1). Compare with this the ornamentation of C. australe 
 (Pl. 32, figs. 1 and 2). The specimen referred to OC. irregulare, from the Walsh River 
 (Pl. 42, fig. 16), has the peculiarly flattened appearance, on its inner or concave side, 
 which generally results from the close contiguity of another whorl, and therein still 
 more indicating its probable relation to O. australe. 
 
 As figured by Mr. Tenison Woods, ©. irregulare is decidedly after the type of 
 Orioceras latus, Gabb,* both in the enrolment of the whorls and form of ornament, but 
 in Gabb’s species the larger prominent ribs are farther apart. 
 
 Loc. Palmer River (The late Rev. J. HE. T. Woods); Head of Walsh River + 
 (Hann's Expedition—Queensland Museum). ; 
 
 * Pal, California, t. 15, f. 25. 
 + The head of the Walsh River is in Paleozoic and Plutonic rocks. Probably the true locality is 
 further down the river. (£R.L.J.) : 
 
502 
 
 Crrocrras, sp. ind., Pl. 83, figs. 4, 5, and 6. 
 Ancyloceras or Hamites, Etheridge fil., Journ. R. Soc. N. S. Wales, 1883, xvii, p. 89, 2nd Pl., bottom 
 Lh. fig. : 
 
 Obs. In 1883 I figured a fragment, provisionally referred to Ancyloceras or 
 Hamites, but which I now think may be more appropriately referred to Crioceras. The 
 ribs are in bundles of two or three, proceeding from a series of single nodes, or tubercles, 
 on the flanks, arranged generally in a line along their centres, or coming close down to 
 the dorsal (concave) margin. Here and there one of the ribs may be much stronger 
 than the others (Pl. 33, fig. 4). 
 
 Another specimen has since come to light from the Aramac Well, in which the 
 arrangement is similar generally, but slightly different in detail (PI. 33, figs. 5 and 6). 
 Here the tubercles are farther apart on the flanks ; the ribs more commonly in bundles 
 of two, this subdivision being remarkably well shown on the back, where also a double 
 row of tubercles is visible. Further examples of these specimens, which are perhaps 
 specifically identical, will be welcome. 
 
 Loe. Landsborough Creek, Thomson River, Pl. 33, fig. 4 (Prof. A, Liversidge— 
 Colln. Sydney University); Aramac Well, at two ane and eighty-four feet 
 (S. Sharwood). 
 
 Crroceras Epxrnst, sp. nov., Pl. 30, figs. 8 and 9. 
 
 Sp. Char. Shell simple, of apparently not more than two volutions, in a more or 
 less oval coil; section oval ; dorsal and ventral lobes about equal, and much smaller than 
 the lateral; dorsal and ventral saddles each divided into two branches, which bifurcate. 
 Surface with equidistant, regular ribs, one becoming larger than the others at intervals, 
 separated by equal interspaces; a row of very small tubercles on each side the back. 
 
 Obs. A small and pretty species of this genus, not exceeding three-quarters of 
 an inch in diameter, resembling in the curvature of its shell, the Crioceras irregulare, 
 Ten. Woods, but the size precludes any reference to this species. Had only a single 
 specimen been present it might have passed for the young of that shell, but as the 
 examples are numerous, and constant in their characters, they can only be regarded as 
 adult individuals, and as such are certainly new to the Cretaceous rocks of Queensland. 
 
 C. Edkinsi is associated with a number of other shells, such as a small Lnoceramus, 
 possibly a Nucula, a small crushed Ammonite, of a strongly Gault facies, and casts of 
 univalves, but the latter not in a good state of preservation. It is allied to, and very 
 like Ancyloceras Beyrichii, Karsten,* especially in the simple coiled whorls. 
 
 The name is given in honour of Mr. HE. R. Edkins, who presented the specimens 
 to the Queensland Geological Survey. 
 
 Loc. Well, seven miles east of Mount Cornish Homestead, near Muttaburra, at 
 two hundred and thirty feet below the surface (2. &. Edkins). 
 
 Family—NAUTILID. 
 Genus—NAUTILUS, Bregnius, 1732. 
 (Dissert. de Polythal.) 
 Navritus HEenpERsont, sp. nov. 
 
 Obs. Fine examples were obtained too late for detailed description, but 
 it may be sufficient to say now that they are after the general type of WV. elegans. 
 Named in honour of Mr. J. B. Henderson, M.I.C.E., Hydraulic Engineer to the 
 Queensland Government, who has presented many fossils to the Geological Survey 
 Museum. ‘These will be described later. 
 
 
 
 * Géol. Ancien. Colombie-Bolivarienne, Vénézuela, Nouv.-Grenada et Ecuador, 1886, t. 1, f. 4a. 
 
508 
 
 Loe. and Horizon. Maxwellton, Flinders River, Lat. 20° 45’ S., Long. 142° 
 48’ E. (J. Burkitt); Wellshot Run, Barcaldine, Lat. 23° 55! 8., Long. 144° 25! E. 
 (A. Lymburner) ; Ilfracombe, Lat. 23° 30! S., Long. 144° 45! E. (— Sheehy). 
 
 Sub-King¢dom—VERTEBRATA. 
 
 Class—PIScEs. 
 Order—CHONDROPTERYGII. 
 Family —LAMNID&. 
 
 Genus—LAMNA, Cuvier, 1817. 
 (Régne Animal, ii., p. 126.) 
 
 Lamna Davrestt, Ltheridge fil. 
 Lamna Daviesti, Eth. fil., Proc, Linn. Soc. N. S. Wales, 1888, iii., Pt. 1, p. 159, t. 4, f. 2 and 3, 
 
 Sp. Char. Vertebre four inches high, three-quarters of an inch in length, and 
 with a transverse diameter of more than two inches. Outline of the centrums oval, 
 with a slightly concave surface. Peripheral fissures very narrow and numerous; margins 
 of the centrums prominent and rounded. ‘ 
 
 Obs. The present very remarkable specimen consists of seven vertebra of a 
 Selachian fish, firmly united together, but slightly displaced obliquely from their normal 
 position, and as a whole six inches in length. In all probability, from the difference in 
 the height and transverse measurement, these vertebra had to some extent an oval 
 outline, but this may have been intensified by the oblique displacement they have 
 undergone. 
 
 With our present unsatisfactory knowledge of the remains of this group of fish 
 in bygone periods, it is difficult to decide on a genus for these remains, but there is a 
 general correspondence to the excellent figures given by Agassiz of the vertebre of 
 extinct species of Zamna, for it is quite clear that the whole of each centrum was ossified, 
 as in the family represented by the genus in question. According to Agassiz’s statement 
 as to the number of the peripheral fissures in the anterior, posterior, and abdominal 
 regions of the column, the present specimen would be those of the abdominal. 
 
 It must be the representative of a very large fish. The Australian Museum 
 contains a Carcharodon Rondeletii, about nine feet long, with vertebre the centrums of 
 which are about half the size only of those in this fossil. Judging by these measure- 
 ments, it would appear to Mr. J. Douglas Ogilby, who has kindly gone into the question 
 with me, that we have here the remains of a fish which must have been from eighteen 
 to twenty feet long. 
 
 Loe. and Horizon. Richmond Downs, Flinders River (C. W. De Vis—Colln. 
 
 Queensland Museum, Brisbane). 
 
 LAMNA APPENDICULATA, Agassiz. 
 
 Otodus appendiculatus, Agassiz, Rech. Poiss. Foss., iii., p. 270, Atlas, i lil,, t. 32, £. 1-25. 
 y Eth. fil., Proc. Linn. Soc. N. 8. Wales, 1888, iii., Pt. 1, p. 158, t. 4, f. 1. 
 ree appendiculata, Smith Waodwand Cat. Foss. Fishes Brit. Mus., Pt. 1, 1889, p. 393. 
 Sp. Char. A tooth of the upper jaw, nearly one inch in height from a line 
 drawn between the fangs upwards to the apex, three-quarters of an inch across the root, 
 
504 
 
 and rather less between the fangs. The upper margin of the root describes almost an 
 ellipse, the fangs being thick and obtusely rounded. The crown is rather more 
 than half an inch high, rather flattened on the inner surface, and gently arcuate 
 from before backwards, with the lateral or cutting edges and the apex sharp. 
 The basal cusps are small, but prominent and sharp, the posterior of the two being 
 the larger. 
 
 This tooth is in all probability from the upper jaw, and from its arcuate outline 
 somewhat posterior in position. The specimen was carefully compared with a large 
 series of similar teeth from the Cretaceous rocks of England, and found to agree 
 excellently with Agassiz’s species, especially that form represented in his Pl. 82, f. 15, 
 the present example being but slightly more arcuate. 
 
 Loc. Limestone at Kamilaroy, Leichhardt River, North-west Queensland 
 (2. L. Jack). 
 
 Order—GANOIDEL. 
 Family—ASPIDORHYNCHID &. 
 
 Genus—ASPIDORHYNCHUS, Agassiz, 1833. 
 (Rech. Poiss. Foss., ii., Pt. 2, p. 135.) 
 
 Obs. Mr. R. Etheridge, F.R.S., has recorded* the caudal portion of the vertebral 
 column, and several of the peculiarly elongated scales of this genus. It is possible, 
 however, that these fragments may belong to the following genus. 
 
 Loc. Hughenden (Lhe late R. Daintree). 
 
 Genus—BELONOSTOMUS, L. Agassiz, 1844. 
 (Rech. Poiss. Foss., ii., Pt. 2, p. 140.) 
 
 Brtonostomus Sweet, Hth. fil. and A. S. Woodw. 
 Belonostomus Sweeti, Eth. fil. and A. 8. Woodw., Trans. R. Soc. Vict., 1892, ii. (2), Pt. 2, p. 1, t. 1. 
 
 Obs. For a full description of the remains of this fish the Reader is referred to 
 the Paper by Mr. A. 8. Woodward, F.Z.S., and the Writer. It is believed to be the 
 largest species of the genus, measuring one*foot three inches in length. It was a much 
 less slender fish than the typical Jurassic species, B. tenuirostris, Ag., and B. sphyrenordes, 
 Ag.,and the superficial ornament of the scales was much more conspicuous and elaborate. 
 The only Belonostomus which appears to be at all comparable to the Queensland species 
 is the large B. Comptoni, Ag., sp., from Brazil, the scale sculpture of the latter being 
 equally conspicuous with our species, with this exception, that the principal flank scales 
 never appear to exhibit the prominent, fine, transverse striations so characteristic of 
 the hinder margin of all the flank scales of B. Sweet. 
 
 Belonostomus lived in the same geological periods in Europe, India, and Brazil, 
 and its discovery in Queensland is thus of great interest, as extending still further the 
 ascertained geographical range of the genus during Mesozoic times. 
 
 Loc. Hughenden (G@. Sweet—Colln. Sweet; and D. P. Ryan—Colln. Geological 
 
 Survey, Queensland). 
 
 
 
 * Quart. Journ. Geol. Soc., 1872, xxviii, p. 346, 
 
505 
 Class—ReEPTILIA. 
 
 Order—CHELONIA. 
 Family—CHELONID 
 
 Genus—NOTOCHELONE, Lydekker, 1889. 
 
 Notochelys, Owen (non Gray), Quart. Journ. Geol. Soc., 1882, xxxviii., p. 178. 
 Notochelone, Lydekker, Geol. Mag., 1889, vi. (3), p. 325. 
 AN Lydekker, Cat. Foss. Reptilia and Amphibia Brit. Mus., Pt. 3, 1889, p. 70. 
 
 NovocHELONE Costata, Owen, sp. 
 Notochelys costata, Owen, loe. cit., p. 178. 
 », Eth. fil., Geol. Mag., 1886, iii., p. 329. 
 Natachelone costata, Lvdekicey. loc. cit., pp. 325 and 70, 
 
 Obs. The remains of this Chelonian consist of the anterior part of the carapace 
 and plastron. These portions were not united by bone, so that no affinity can exist with 
 the freshwater and terrestrial genera. It appears to be more nearly allied to the marine 
 Turtles (Chelone). . 
 
 Sir Richard Owen states this to be the first evidence of a fossil Chelonian 
 obtained in Australia, but he appears to have overlooked the late Mr. Krefft’s discovery 
 of the carapace of a freshwater species in the Wellington bone-caves * and Dr, E. P. 
 Ramsay’s description of the pelvis of a Turtle from Lord Howe Island.+ 
 
 Furthermore, a marginal scute of a Chelonian from Westbrook, a tributary of 
 Oakey Creek, Condamine River, has long been in the collection of the Geological 
 Department of the British Museum, presented thereto by Dr. G. Bennett. 
 
 The district in which this interesting fossil was found abounds in organic remains 
 of Cretaceous age, and there is nothing in the structure of this Chelonian which would 
 militate against its having lived at that period of the earth’s history. 
 
 Loc. Landsborough Creek, Thomson River (Prof. A. Liversidge—Colln. 
 Sydney University). 
 
 Order—ICHTHYOPTERYGIA. 
 
 Genus—ICHTHYOSAURUS, Konig, 1820. 
 (Icon. Foss. Sectiles, t. 19, f. 250.) 
 
 IcHTHYOSAURUS AUSTRALIS, MeCoy. 
 
 Ichthyosaurus australis, McCoy, Ann. Mag. Nat. Hist., 1867, xix., p. 855; Ibid., xx., p. 196. 
 4 o McCoy, Trans. R. Soc. Vict., 1868, viii., Pt. 1, p. 42; Jbéd., 1869, ix., Pt. 2, p. 77. 
 + 7. Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 228. 
 
 Sp. Char. Centrums of the vertebrae four inches wide, three inches deep, and one 
 and a-half inches long, deeply biconcave, and with conical articular surfaces; paddles 
 with eight rows of phalangeal joints ; teeth with a rough, bony, square base, above which 
 the smooth base of the crown has a circular section, the remainder of the conical crown 
 being marked with close irregular obtuse ridges, with narrow intermediate impressed 
 lines; eyes five and a-half inches in antero-posterior diameter, the pupillary opening two 
 inches, and the sclerotic divided into about thirteen pieces. (MeCoy.) 
 
 Obs. This is said by Sir F. McCoy to be one of the largest species of the genus, 
 being twenty-five feet long. The teeth resemble those of I. campylodon, Carter, from 
 the English Chalk. 
 
 * Australian Vertebrata, Foss. and Recent, 1871, p. 39. 
 + Proc. Linn, Soc. N. 8. Wales, 1882, vii., Pt. 1, p. 86. 
 
506 
 
 It would be a great boon if Prof. McCoy would publish a full description of this 
 interesting Reptile, as quite recently fine additional remains of J. australis have come to 
 hand through the labours of Messrs. J. Burkitt, J. Hugh Moor, and W. L. Mackinnon. 
 The first of these gentlemen has obtained the snout portion of a large head with powerful 
 teeth and a number of united vertebre; the second a portion of a skull showing the 
 orbit, with sclerotic plates in situ, and a large number of disjointed centrums of vertebra ; 
 whilst the last-named collector has forwarded other disarticulated centrums, which, 
 although smaller, have every appearance of being those of this species. 
 
 Loc. Base of Walker’s Table Mountain, Flinders River (Messrs. Carson and 
 Sutherland—Nat. Mus., Melbourne); Bed of Flinders River, thirty-five miles below 
 Richmond Downs, approximately Lat. 20° 37’ S., Long. 142° 43’ E. (J. Burkitt) ; 
 Flinders River, at Manfred Downs, approximately Lat. 20° 5’ S., Long. 141° 45' E. 
 (J. Hugh Moor) ; Glendower, Upper Flinders (W. L. Mackinnon). 
 
 IcHTHYOSAURUS MARATHONENSIS, Etheridge fil. 
 Ichthyosaurus marathonensis, Eth. fil., Proc. Linn. Soc. N. 8. Wales, 1888, iii., Pt. 2, p. 405, t. 7. 
 
 Obs. The fossil consists of that part of the upper and lower jaws of a large skull 
 anterior to the nostrils. It measures ten inches in length, and exhibits the greater 
 portion of the right maxillary and dentary bones, and a portion of the left. At the 
 anterior end the specimen has been broken off short, immediately posterior to the union 
 of the rami, and at the hinder end just anterior to the outer termination of the nasal 
 bones. At the former the snout is three and a-half to four inches in transverse measure- 
 ment, and at the latter point four and a-half inches. There are thirty teeth in all 
 preserved, ten implanted in the pre-maxillary, and eleven in the dentary. 
 
 Both bones are longitudinally channelled by a deep semi-interrupted groove, 
 similar to that seen in other species of Ichthyosaurus. 
 
 The teeth are of medium size, but larger than in some species, measuring from an 
 inch to an inch and a-quarter from the alveolar edge to the apex of the crown, but 
 including the implanted base, one of the foremost teeth measures an inch and three- 
 quarters in length. They increase in diameter and stoutness from before backwards, are 
 conical sub-circular in section, with a non-trenchant and apparently straight crown. The 
 enamel is ornamented with grooves and ridges, but there is no evidence that the crown 
 apices were devoid of these; but, on the contrary, the upper portions of the crown and 
 the base of the teeth above the alveolus appear to be more strongly ridged than does the 
 middle line of each tooth. In the most anterior tooth but one preserved in the 
 pre-maxillary, having a sectional diameter of half an inch, there is a pulp cavity of 
 three-sixteenths of an inch. 
 
 In a transverse section of the posterior end the following facts are discernible. 
 The breadth of the pre-maxillary across the top of the alveolar cavity is one inch. On 
 the outer border the external groove traversing this bone longitudinally leads into a 
 well-marked cavity, the exterior alveolar wall being thin, but this is perhaps owing to 
 some extent to the lateral abrasion the specimen has undergone. The alveolus cut by 
 the section is five-eighths of an inch wide and an inch in depth. From the thickened 
 and enlarged lower end the inner wall of the bone is directed upwards in a fairly 
 straight line until it reaches a point on a level with the upper end of the alveolus. Here 
 it takes a well-marked bend inwards to above the cavity of the external groove; thence 
 it bends outwards to become the median surface for union with that of the left pre- 
 maxillary. The inner alveolar wall descends at least four-eighths of an inch lower than 
 the outer one. There is no indication of the nasals. In the lower jaw the lower portion 
 of the dentary is not preserved, having flaked off from the specimen, but this bone 
 
507 
 
 would probably present a deeply sigmoidal outline if whole. It now measures through 
 the base of the alveolus an inch and one-eighth, the latter being six-eighths of an inch 
 deep. From the bottom of the alveolus through the inner portion of the dentary there 
 is only a thickness of three-sixteenths of an inch. The upper element of this bone is 
 nearly as correspondingly thick as the lower portion of the pre-maxillary, whilst that 
 part below the alveolus, including the portion split off, is at’ least one inch in height. 
 The external longitudinal groove leads into a sac, which, with the passage uniting the 
 latter to the outer groove, almost completely cuts the bone itself in half, and strongly 
 resembles the similar vascular canal in the pre-maxillary. We also notice in this section 
 the difference in the angle of the alveolus in the upper and lower jaws, and doubtless 
 the curved outline of the lower teeth is a provision of nature to bring them into 
 apposition with those of the upper jaw, which are straighter and set at an entirely 
 different angle. 
 
 Ido not see any trace of the splenial bones, the fracture which severed this 
 portion of the jaws from the remainder of the head having taken place too far forward, 
 unless the small fragment of bone at the very bottom of the section in the middle 
 line represents the anterior termination of the right splenial. 
 
 Since Prof. Sir F. McCoy’s first announcement of Enaliosaurian remains in 
 Queensland very little seems to have been done towards working out the distribution of 
 this important group of reptiles in Australia. The details of his Ichthyosaurus australis 
 given by McCoy are so meagre that it is with the greatest difficulty a comparison can 
 be instituted with any other remains. The presence of the casts in the Australian 
 Museum would have rendered this task easier than it otherwise could have been had 
 that portion of the head mentioned by McCoy as bearing teeth been present, but the 
 cast in the Museum consists of a portion of the right side included between the 
 posterior margin of the orbit to about half the length of the nostrils, measuring one 
 foot in length by seven and a-half inches high. This portion of the cranium is, of 
 course, much posterior to that bere described, but, judging from the relative pro- 
 portions of the two specimens, I am inclined to regard the present fragment as a 
 portion of a species quite as large as Sir F. MeCoy’s, and it is possible they may be 
 identical. 
 
 The general proportions of this snout resemble those of I. campylodon, Carter, 
 from the English Chalk, and there is present in this species a well-marked vascular 
 channel * along the pre-maxillary and dentary bones, just as we see it here. Describing 
 this, Sir Richard Owen says: ‘‘ Opposite the origin of the inner alveolar plate the pre- 
 maxillary is traversed by a straight longitudinal groove, four lines in breadth, which 
 contracts as it advances forwards.”+ Touching the similar groove seen along the 
 dentary, he adds: ‘“ The outer part of the dentary at the hinder fracture is six lines in 
 thickness, smooth, and convex on its outer side, which is traversed by a longitudinal 
 groove, which also slightly narrows as it advances.” 
 
 As well as in I. campylodon, this groove is shown in Sir R. Owen’s figures of the 
 jaws of I. communis t and I. platyodon,§ Liassic species. 
 
 Sir F. McCoy notes the resemblance of the teeth of his I. australis to those of 
 I. campylodon, previously referred to, a likeness which is also perceptible in our species. 
 I am unable, however, to institute a comparison between the latter and J. australis, 
 from the fact that the casts in the Australian Museum do not exhibit the teeth. 
 
 
 
 * Mon. Foss. Rept. Cret. Form., 1851, t. 25, fig. lg. 
 + Loc. cit., p. 75. 
 
 + Mon. Foss. Rept. Liassic Form., t. 24, f. 2. 
 
 § Ihid., t.. 31, f, 2. 
 
508 
 
 The upper surface of the pre-maxillary, judging from the section of the right 
 one, would form rather a narrow arch, differing very much in this respect from the 
 broad semi-circular outline of L. campylodon. 
 
 In describing the Fossil Reptilia of New Zealand, Sir James Hector, F.R.S., 
 has applied the name of Zchthyosawrus australis* to some remains found in that 
 country. Sir F. McCoy’s name having priority, that of the New Zealand species will . 
 need alteration. 
 
 Loc. Marathon Station, North-Central Queensland (C. W. De Vis—Queensland 
 Museum, Brisbane). 
 
 
 
 Order—SAUROPTERYGIA. 
 
 Genus—P LESIOSAURUS, Conybeare, 1821. 
 (Trans. Geol. Soc., v., Pt. 2, pp. 560 and 581.) 
 
 PLESIOSAURUS MACROSPONDYLUS, McCoy. 
 Plesiosaurus macrospondylus, McCoy, Ann. and Mag. Nat. Hist., 1867, xix., p. 356; Ibid., xx., p. 196. 
 %9 5 McCoy, Trans. R. Soc. Vict., 1868, viii., Pt. 1, p. 42. 
 
 Sp. Char. Cervical vertebre only known ; each centrum three inches long, three 
 wide, and two and a-half inches deep. (McCoy.) 
 
 Obs. Sir F. McCoy remarks that this appears to be specifically distinct from 
 P. Sutherlandi, by the extraordinary rugosity of the edges of the articular ends of the 
 centrum, as in Plesiosaurus rugosus, each of which presents a remarkably elongated form. 
 Our present knowledge of P. macrospondylus is very inadequate. 
 
 Loc. Base of Walker's Table Mountain, Flinders River (Messrs. Carson and 
 Sutherland—N ational Mus., Melbourne). 
 
 PLESIOSAURUS SUTHERLANDI, McCoy. 
 
 Plesiosaurus Sutherlandi, McCoy, Ann. and Mag. Nat. Hist., 1867, xix., p. 856; bid., xx., p. 196. 
 £ McCoy, Trans. R. Soc. Vict., 1868, viii., Pt. 1, p. 42. 
 3 es Eth. fil., Ann. Report Dept. Mines N. 8S. Wales for 1887 [1888], p. 167, Pl. 1, f. 1-4. 
 
 Obs. Sir F'. McCoy has very briefly described the trunk vertebre of this reptile— 
 too briefly for his remarks to be of much service in determining the species. He states 
 that the length of the centrum is two and a-quarter inches, the width three and three- 
 quarters, and the depth two and a-half inches. These measurements, Prof. McCoy 
 thinks, resemble those of P. australis, Owen, from New Zealand, but the proportions are 
 obviously different. 
 
 Thanks to the kindness of Sir F. McCoy, in forwarding his original specimens 
 for comparison, I have been able to identify with his species some additional remains 
 from Central Queensland. The fossils consist of the centrums of cervical vertebre, 
 without processes. They are transversely ovate or ellipsoidal in outline, two and an eighth 
 inches long, four and a-half wide, and two and three-quarters high. The upper surface 
 is depressed convex, but below the middle line is sub-angular. The venous openings _ 
 are two, large and distinct, the surface of the vertebre exterior to them, and between them 
 and the pleure, more or less concave. The centrums havea well-marked, rather flattened 
 articular surface, half an inch wide, but with sharp, erect, non-rugose external edges. 
 Within the articular surface each centrum is depressed, but not actually concave, in 
 fact more flattened than concave, three inches by one and a-half, smooth, and with the 
 faintest trace of a tubercle or prominence. ‘The neurapophysial and pleurapophysial 
 surfaces are contiguous to one another ; and the last-named, although lateral in position, 
 
 
 
 * Trans. N. Zealand Inst. for 1873 [1874], p. 155. 
 
 
 
509 
 
 are nearer to the upper than the lower surfaces of the centrums, and they in no way hide 
 any part of the inferior surfaces of the latter. The neurapophysial surfaces were long 
 fore and aft, and somewhat narrow, but those of the pleurapophysial, on the other hand, 
 were large and oblique, and somewhat narrow. 
 
 In P. australis, Owen, there are two large and two small venous foramina instead 
 of only two large, as in the present case. Amongst other New Zealand species is P. 
 erassicostatus, Owen,* the centrums of which, according to Sir James Hector, “are deeply 
 excavated beneath, with two venous foramina. The articular surfaces are elongately 
 transverse, forming a contracted oval, and only moderately concave with rounded 
 margins.’’+ In the Queensland bones the margins are distinctly flattened, and the 
 ventral surface, instead of being excavated, is convex. The concavity mentioned by 
 Hector is visible in his figures, and gives a character to the vertebre not to be mistaken 
 or overlooked. Furthermore, the centrums of the former have no definite tubercle, 
 which is present in P. crassicostatus. 
 
 Loc. Walker’s Table Mountain, Flinders River (Messrs. Carson and Suther- 
 land—National Mus., Melbourne); Pitchery Creek, Barrington’s Station, Central 
 Queensland (A. J. W. Crummer—Mining and Geol. Mus., Sydney); Marathon 
 (G. Sweet—Colln. Sweet, Melbourne). 
 
 Some additional remains of Plesiosaurus have lately been described by the Writer,t 
 consisting of vertebre and ribs confusedly intermingled. No good purpose would be 
 served by applying names to these bones, but the following is a general description of 
 the fossils. 
 
 Tn this mass we have the remains of at least four vertebra, which, judging from the 
 form and attached processes, are clearly those of the dorsal series. Only one, however, 
 is in any degree perfect, the others having undergone fracture, and all abrasion. 
 Intermingled with the vertebre are portions of ribs, particularly two well-marked 
 fragments, and an articular end of a third. 
 
 The most perfect vertebra is five and a-quarter inches high, but the inferior 
 margins of the centrum are not preserved, so that this measurement is somewhat under 
 that of the perfect size of the bone. The edges of the articular surfaces are much 
 worn and decorticated, but, as preserved, the entire centrum is an inch and a-half in 
 height, and the concave articular surface an inch and a-quarter. The length of the 
 centrum, fore and aft, is an inch and three-quarters, and the breadth, or width, two 
 inches. The neural spine, from the upper margin of the canal in the middle line, is 
 three and three-quarter inches in height, but is shortened by fracture ; it is sharp, thin, 
 and laterally compressed. At its base the spine is an inch and a-half thick from before 
 backwards ; but at the broken upper extremity, the transverse width is a little less than 
 aninch. It is very erect, and does not appear to have any posterior inclination, , but 
 the posterior zygopophysis would overhang the succeeding centrum to a slight extent 
 when in apposition with it. The neural canal itself is broadly oval, measuring an inch 
 in its longest diameter; but the pre-zygopophysis is not preserved. The diapophysial 
 support of the rib visible is placed very high up, and is directed backwards and upwards 
 and forms the entire costal surface; below this point the surface of the vertebra is 
 much hollowed. .The diapophysis is ledge-like, flattened to some extent above and below, 
 
 
 
 * Geol. Mag., 1870, vii., p. 53. 
 
 + Trans. N. Zealand Inst., 1874, vi., p. 342. 
 
 + On additional Evidence of the occurrence of Plesiosaurus in the Mesozoic Rocks of Queensland. 
 Proc. Linn, Soc. N. S. Wales, 1888, iii., Pt. 2, p. 410, t. 8. 
 
510 
 
 with the ridge connecting its under portion to the lateral surface of the centrum very 
 ill-defined. The actual surface for the rib-articulation is not preserved, through 
 fracture. 
 
 The remains of the ribs consist either of portions of two or else one broken in 
 half with the severed ends contiguous to one another. One of these pieces is six inches 
 in length, the other six and a-half inches, the former practically straight, the latter 
 curved, and both laterally compressed. When united these would represent a rib from 
 thirteen to fourteen inches long. The third example, previously referred to, represents 
 the proximal end of a rib, with a simple expanded termination about three-quarters of 
 an inch in diameter. 
 
 Taking into consideration the general character of these bones and the position 
 of the diapophyses, little doubt can be entertained that we are - dealing with vertebrae 
 of the dorsal series. In describing those of Plesiosaurus dolichodeirus, Conyb., Sir. R. 
 Owen says—“ The transition from the cervical to the dorsal series is effected by the 
 usual elevation of the costal surface by gradational steps continued through about five 
 vertebrx, until a single costal surface is presented by a large diapophysis from the 
 neural arch.’’** This is precisely what we have here, the diapophysis assuredly having 
 reached its definite elevation. Again, if I am right in conjecturing that the two pieces of 
 rib appertain to one, the sum of these characters would seem to indicate the middle of the 
 dorsal series, as the position to be occupied by the present bones when zw sitw in the 
 column. 
 
 Little can be said as to the specific identity of these vertebre, but we cam only 
 compare them with those of the preceding species :— 
 
 “P. macrospondylus, McCoy.— Cervical vertebree with very rugose articular 
 surfaces to the centrum.” 
 
 “ P. Sutherlandi, McCoy.— Trunk’ vertebre, having the centrum two and a-quarter 
 inches long, by three and three-quarter inches wide, by two and a-half inches deep.” 
 
 As regards the first of these vertebra, they are, so far as discovered, cervical, but 
 if the dorsal are similarly rugose, the bones now under description must be distinct. In 
 connection with P. Sutherlandi, the word “ trunk’? would lead one to infer that dorsal 
 vertebre are probably meant, as distinct from cervical and caudal; if so, the measure- 
 ments are quite different from those of the present specimens. 
 
 Several species have been described from the Mesozoic rocks of New Zealand by 
 Sir R. Owen, F.R.S.,¢ and Sir James Hector, F.R.S.; { but I am unable to satisfy myself 
 of the identity of the present specimens with any of them. Two, P. australis, Owen, 
 and P. crassicostatus, Owen, appear to be well known. The first is distinguished by 
 the general character of its vertebre ; and the second by the presence of a very large 
 central tubercle. The four others we are less acquainted with, and a comparison without 
 actual specimens becomes very difficult. Two, P. Hoodi, Hector, and P. Holmesit, 
 Hector, are known only by cervical vertebre; whilst of the two others, P. Traversi, 
 Hector, and P. Mackayi, Hector, we are only acquainted with cervical vertebre and 
 portions of the lower jaw of the first, and general fragments of the skeleton of the 
 second. Under these circumstances, as I am unable to make as minute comparisons as 
 should be done, a distinctive name is not applied to the fossils now under consideration. 
 
 Loc. Walsh River, North Queensland (C. W. De Vis—Queensland Museum, 
 Brisbane). 
 
 EK. 
 
 * Mon. Foss. Reptilia Lias Form., 1865, Pt. 1, p. 6. 
 + Report Brit. Assoc., 1861, p. 122; Geol. Mag., 1870, p. 52. 
 { Trans. N. Zealand Institute for 1878 [1874], p. 333. 
 
CHAPTER XXXIIT. 
 
 THE DESERT SANDSTONE FORMATION. 
 (UPPER CRETACEOUS.) 
 
 Tuts great formation must at one time have covered at least three-fourths of the 
 Colony of Queensland, although its denuded remains now occupy less than the twentieth 
 part of the area over which it originally extended. After the Rolling Downs Formation 
 had been laid down in the comparatively narrow sea which connected the Gulf of 
 Carpentaria with the Great Australian Bight, and converted the Australian area into 
 two islands, a considerable upheaval took place. The denudation of the Rolling Downs 
 Formation followed, and must have gone on for some time. Unequal movements of 
 depression then brought about lacustrine conditions on portions of the now uplifted 
 bottom of the old deep-sea strait, and in other portions permitted of the admission of 
 the waters of the ocean. Finally, a general upheaval placed the deposits of the period 
 just concluded in nearly the positions in which we now find them. 
 
 In the southern portion of the Colony a good deal of the Desert Sandstone may be 
 seen without leaving the Southern and Western Railway. It begins first to arrest the 
 attention of the traveller to the west of Hodgson, in the low table tops of Mount Abun- 
 dance, near Brinsop Railway Station (338 miles). The station is 1,170 feet above the sea, 
 and the base of the sandstone tableland is not much above that altitude. The railway cuts 
 through a low sandstone tableland, about the same altitude, just before reaching Amby 
 Station, and passes to the south of another on the opposite or west bank of Amby Creek. 
 South of Mitchell Station (1,104 feet), another sandstone tableland is passed on the north. 
 Between Womallilla and Mungallalla Stations (400 miles) the line cuts through another 
 tableland which stretches for a considerable distance to north and south.* At Dulby- 
 dilla (410 miles) the line surmounts the divide between the Culgoa and Warrego Rivers, 
 which is capped by a table of Desert Sandstone about two hundred and eighty feet in 
 total thickness, the upper portion being red, gritty, ferruginous, and the lower portion 
 felspathic sandstone. The base of the sandstone is only a little above the level of 
 Dulbydilla Railway Station (1,443 feet). One standing on the top of the range near 
 Dulbydilla, and looking north and east, can see the Desert Sandstone forming an almost 
 continuous line of cliffs enclosing, like a frame, the heads of the Culgoa River, and 
 prolonged eastward along the summit of the so-called “Great Dividing Range” between 
 the Dawson and Condamine Rivers. In the sandstone at Dulbydilla—which I have had 
 an opportunity of examining minutely +—I saw no organic remains except plant- 
 impressions, too imperfect for identification. At 398 miles (two miles east of Mun- 
 gallalla Station), a fine-grained ferruginous sandstone, red to yellow in colour, yielded a 
 number of curious impressions, to which Mr. John Falconer directed my attention, and 
 
 
 
 * Tt is evident from the descriptions given by the late Rev. W. B. Clarke of the localities from which 
 the Wollumbilla and Amby fossils were derived, that he had no idea that the sandstone tablelands in question 
 were distinct from the fossiliferous (Rolling Down) beds, an idea which the late Mr. Richard Daintree was 
 the first to entertain. 
 
 + In October, 1885, when on an expedition in search of artesian water in the Western Interior, in 
 
 company with the Hydraulic Engineer, 
 
512 
 
 which are in the Survey Museum awaiting the advent of somebody who can throw light 
 upon their origin. The surface of the sandstone, which is in thin flags, is marked by a 
 network of raised lines crossing one another at all angles. These lines are probably due 
 to the filling up, with fine sand, of cracks produced by sun-drying, the subsequent 
 shrinking of the rock on consolidation having left the lines standing in relief. Hach 
 square, or rectangle, or trapezoid, encloses a scroll in high relief, the outer end of which 
 generally springs from one of the straight lines. The scrolls somewhat resemble the 
 circinate vernation of the fronds of ferns, but the resemblance is evidently a mere fancy- 
 My Colleague believes that the scrolls are not even of organic origin, and they form an 
 unsolved puzzle which weighs on my mind. At this place the Desert Sandstone rises to 
 a height of about one hundred feet above the level of the railway. The highest beds are 
 of red sandstone. ‘These rest on yellow sandstones, which overlie shales or mudstones, 
 with bands.of clay-band ironstone nodules. It is on the yellow sandstones that the 
 circinate markings occur. The same beds also contained tracks and burrows, and 
 questionable plant-remains, including fragments of silicified wood. 
 
 The railway line furnishes a convenient datum from which the altitude of the 
 base of the Desert Sandstone can be ascertained. So far as the railway traverses the 
 district of Maranoa—.e., from Yeulba (281 miles) to Dulbydilla (410 miles)—it rises 
 with a gentle grade from 986 feet to 1,443 feet above the sea-level, or about six 
 feet in a mile. The bases of the Desert Sandstone fragments seen from the railway 
 probably average about twenty feet above the level of the rails. In other words, the 
 present denuded surface is only a little below that on which the Desert Sandstone was 
 laid down. The base of the Desert Sandstone may be taken to rise from 1,006 feet at 
 Yeulba to 1,463 feet at Dulbydilla. 
 
 Over the whole Maranoa District the Desert Sandstone rests horizontally, and 
 with a distinct unconformability, on the Rolling Downs strata, which dip to the south, and 
 from which the Wollumbilla fossils discovered by Mr. Gordon and described by the 
 Rev. W. B. Clarke in 1867,* and by Mr. Charles Moore + in 1869, the fossils described 
 by the latter gentleman from the Amby River, Mount Abundance Run, Blythesdale, and 
 Bungeworgorai,{ and the fossils from the Mitchell River, and Roma, collected by me in 
 1885, and described by my Colleague in the following pages, were collected. 
 
 My journey to the west in 1885 led me from the then terminus of the railway 
 (Dulbydilla) to the present terminus at Charleville by coach. From Dulbydilla to 
 Morven (nineteen miles), the soil is red and sandy, and is evidently derived from the 
 decomposition of the Desert Sandstone, although the latter is probably zn situ only on 
 the very divide. An outlying table of Desert Sandstone is seen on the north side of 
 the road. From Morven to Thurles (fifteen miles), the soil is reddish, but gradually 
 grows greyer to the west. At Thurles (1,250 feet), the surface is strewn with pebbles 
 of red sandstone and red ironstone, derived from the decomposition of the Desert Sand- 
 stone. A Desert Sandstone tableland lies north of the road between Hamburgh and 
 Angellalla Creeks. A large tableland, known as the Angellalla Range, lies between 
 Angellalla and Bradley’s Creeks. Its base is 1,360 feet, and its summit 1,485 feet above 
 the sea-level. The upper beds are coarse and gritty with quartz pebbles; the lower 
 beds are hard, white, fine-grained and felspathic, with a conchoidal fracture. 
 
 From the Angellalla Tableland to Charleville only the “ Rolling Downs” strata 
 are met with. The level of Charleville by the railway survey is nine hundred and 
 sixty-six feet. When Mr. J. B. Henderson, Hydraulic Hngineer, and I travelled 
 
 
 
 * Quart. Journ. Geol. Soc., 1867, xxiii., p. 7. 
 + Loc. cit., 1870, xxvi., p. 226. 
 t Loe. cit., p. 233. 
 
513 
 
 together in 1885 the Aneroid gave the level of Charleville as 1,190 feet. Although the 
 latter reading must be wrong, it may be. retained for the sake of comparison, as it 
 was one of a series taken all along the route from Brisbane to the Grey Range. At 
 Millie Station, on the Ward River, our Aneroid read 1,120 feet. The southern 
 extremities of Desert Sandstone tablelands were seen to the north of the Adavale 
 road, between the Nive and Ward Rivers, and between the Ward River and Middle 
 Creek. The bases of these tabl elands would probably be about 1,200 feet above the 
 sea, by our reckoning. 
 
 Between Ambatalla Creek (1,190 feet) and Emu Creek (1,025 feet) the road 
 crosses a Desert Sandstone tableland (the Paroo Range), which extends from north to 
 south and is seven miles in breadth. The base of the sandstone is 1,080 feet and its 
 summit 1,280 feet above the level of the sea. The difference in the vegetation of the 
 tableland and of the surrounding “ Rolling Downs” is most marked. The ‘“ Downs”’ 
 are well grassed and covered in places with mulga and gidyah trees, while the Desert 
 Sandstone has only low brushwood and is almost destitute of grass. The Paroo Range 
 is a spur of the Warrego Range, which divides the heads of the Bulloo River from the 
 heads of the Barcoo. Opals are said to be abundant in the range at the head of 
 Pleasant Creek. I have been reliably informed that the northern part of the range 
 is capped by a lava-form bed of basalt. 
 
 The Town of Adavale (1,000 feet) is built on a cemented gravel or cong!omerate, 
 apparently derived from the waste of the Desert Sandstone. 
 
 Between Adavale and Milo Station, on the Bulloo (fifteen miles north-north- 
 west of Adavale), is a low tableland of Desert Sandstone. About two miles north of the 
 station a spring rises from a fine-grained hardened sandstone rock (Desert Sandstone ?), 
 and even in the terrible drought which prevailed at the date of our visit gave an estimated 
 yield of one and a-haif cubic inches per second. This spring is about 1,030 feet above 
 the sea and twenty feet above the station. At the base of the Desert Sandstone table- 
 land, west of the station, the Manager, Mr. Beck, informed me that there are springs 
 eapable of watering four thousand sheep in the driest season. In a well in the north- 
 west corner of Britomart Block, thirty miles west-south-west of Milo Station, a well was 
 being made through the Desert Sandstone. The section was described by the sinker as 
 follows :— 
 
 Feet. 
 Yellow and brown sandstone [Desert Sandstone] .. : ... 138 
 Blue-grey clay shales, with indistinct plant remains [Rolling Downs] 19 
 
 157 
 Brackish water was met with at fifty feet ; the supply is only about six hundred gallons 
 per day. 
 
 The direct road from Adavale to Windorah, on the Thomson River, crosses the 
 Desert Sandstone tableland in Lat. 25° 50'S. North of the road the tableland bifurcates, 
 the western limb being known as the Cheviot Range, and the eastern limb retaining the 
 name of the Grey Range. The public-house ‘“ Jack on the Rocks’ affords a weleome to 
 the weary bushman near the summit of the range, although rather on the Barcoo fall. 
 A shallow well near the house collected, even in the terrible drought of 1885, sufficient 
 soakage water from the Desert Sandstone to supply the house. Mr. Beck informed me 
 that springs break out—(1) At the base of the sandstone at the bifurcation of the Cheviot 
 and Grey Ranges (head of Coonabiila Creek) ; (2) in Oxford Downs Block, halfway up 
 the range; (3) in the same block on the top of the range; (4) at the base of the Grey 
 Range, near the head of Durilla Creek; and (5) round the base of an isolated tableland 
 
 21 
 
514 
 
 between Coorajah and Spencer Creeks (between Grey and Cheviot Ranges). Two of 
 these springs were capable of watering one hundred thousand sheep each, and another 
 of watering twenty thousand, even in the drought of 1885. 
 
 Opals are found in the Cheviot Range, on Bulgrov Run, and in the Grey Range, on 
 Nickavilla Run. At the latter place, Mr. Fitzwalters, of Adavale, one of the owners of 
 the mine, informed me that the opals are found by driving into the conglomerate or 
 sandstone cliffs, the opals being found in nodules of siliceous ironstone. Elsewhere they 
 are found in similar nodules scattered over the surface of the Rolling Downs, and 
 evidently derived from the waste of the Desert Sandstone. Some of the finest opals I 
 have ever seen came from Kyabra Creek, in this neighbourhood. The ‘change in popular 
 fancy” and the “eradication of prejudice’’ which I observed in 1886 * were all that was 
 required to make the Queensland opals “as valuable as the most appreciated gems from 
 Hungary,” appear to have already in some measure been brought about. 
 
 In the whole of the region described, from Dulbydilla to the Grey Range, the 
 Desert Sandstone tablelands rest on the Rolling Downs beds at elevations varying 
 from 1,463 feet to about 1,000 feet The late Mr. Charles 8S. Wilkinson, Government 
 Geologist of New South Wales, informed me, however, that the Paleozoic rocks of the 
 Barrier Ranges are coutinued into Queensland at the southern end of the Grey Range, 
 and it is probable that the Desert Sandstone in that locality rests directly on the Paleozoic 
 rocks. 
 
 West of the Grey Range the Desert Sandstone forms a tableland extending from 
 north to south for nearly one hundred and fifty miles, with a breadth varying from 
 seven to thirty-six miles. [I have not visited this outlier, but it is evident from the Runs 
 Map, published by the Lands Department, that the rainfall soaked up by the Desert 
 Sandstone escapes in springs around its base—that is, as soon as it comes in contact 
 with the argillaceous rocks of the Rolling Downs Formation. The same is true of 
 Willie's, Walter’s, and Hood’s, three little ranges north of Hungerford, and which are 
 surrounded by springs. 
 
 The Desert Sandstone of the Cheviot Range, although it has been breached by — 
 the Thomson River at Windorah, is doubtless continued to the north for nearly two 
 hundred miles by the range which divides the Diamantina waters from those of the 
 Thomson. The south end of this range is unknown to me, but I had an opportunity in 
 January, 1882, of seeing its northern extremity near Winton. It presents a long line 
 of bold mural cliffs to the north, and is surrounded by outlying fragments, once a part 
 of it, to north, south, east, and west. {f visited the “‘ Lancewood Range,’’ between the 
 Diamantina River and Wokingham Creek, and found it to be composed partly of gritty 
 white sandstone and partly of hardened white clay, horizontally bedded. 
 
 In the “Opal Range,” south of Winton, and in the tableland between the 
 Diamantina and Mayne Rivers, both outliers from the long tablelands, opals are found. 
 
 Between Morven and Tambo something is again seen of the Desert Sandstone, in 
 the spurs from the western side of the range dividing the Warrego from the Balonne 
 waters, and of the fragments into which the range has been cut. Seven miles west of 
 Clara Creek is a tableland of horizontal beds of fine-grained hard sandstones, with 
 layers and bands of hardened felspathic clay, presumably the north end of the Angellalla 
 Range already mentioned. The beds have a total thickness of a little less than eighty 
 feet, the road being 1,400 feet and the top of the tableland 1,480 feet above the sea- 
 level. Several fragments of the Desert Sandstone tableland are seen to right and left 
 of the road between Clara Creek and the township of Ellangowan, on the Warrego 
 
 
 
 * Handbook of Queensland Geology, p. 77. 
 
515 
 
 River. The road also crosses several ridges covered with stony débris of the Desert 
 Sandstone, but as a rule it keeps on the lower Rolling Downs Formation. Between 
 Augathella and Nive Downs the road for eight miles is carried over a red sandy ridge, 
 obviously formed from the débris of the Desert Sandstone, which is probably in situ 
 The road up the right bank of the Nive River shows nothing but the Rolling Downs 
 Formation, and the divide between the heads of the Nive and Barcoo is crossed almost 
 imperceptibly, and Tambo is reached without the Desert Sandstone being met with, 
 although its cliffs are seen in the distance to left and right. 
 
 As the road from Tambo to Blackall follows the course of the Barcoo River below 
 the level of the base of the Desert Sandstone, nothing of that formation is seen, but 
 there can_be no doubt the “ Broken Sandstone Ridges,’ seen in the distance towards 
 the heads of Dismal, Birkhead, and Windeyer Creeks, and which are laid down on the 
 Runs Map of Mitchell District, issued by the Lands Department, are outliers of the 
 Desert Sandstone Range, between the heads of the Bareoo and Belyando. The Runs 
 Map of Mitchell District shows the edge of the Desert Sandstone tableland east of 
 Aramac, and also shows distinctly how the water absorbed by the porous sandstone 
 escapes at the edge of the tableland to form springs and waterholes (Friendly Springs, 
 Lake Mueller—a soda lake—&c). On the Blackall and Aramac Road, between Home 
 and Evora Creeks, the country is sandy, and the southern half of the district is covered 
 with blocks of stone derived from the Desert Sandstone, clothed with Spinifex grass 
 (Triodia) ; but the Rolling Downs strata are the rocks in situ. - It is evident, however, 
 that the Desert Sandstone has but recently been denuded from this locality. The 
 crossing of the Alice near Evora Creek is 1,150 feet above the level of the sea.* 
 
 The road from Blackall to Jericho Railway Station, which was the terminus of 
 the Central Railway when I visited the district in November, 1885, after the first 
 twenty-five miles up Dismal Creek, is carried through heavy sand clothed with Triodia, 
 evidently the débris of Desert Sandstone; bunt it is at fifty-six miles from Blackall that 
 the formation is first seen in situ at a place locally known as “The Rocks.” The 
 sandstones are hard, fine-grained, yellow, ferruginous, and micaceous. Three miles 
 further low hills rise on the north to an elevation of 1,930 feet above the sea and 50 
 feet above the road. The beds of which these hills are composed dip at 3° to the 
 west. <A continuous cliff-section could not be seen. The uppermost beds are, of course, 
 hard yellowish grit (which would make a fine building stone) with imperfect plant- 
 impressions, and a beautiful fine-grained, hard, white, siliceous grit, with a vitrified 
 appearance. One piece of a silicified tree which | saw lying flat on the grit was three 
 feet long and about eight inches in diameter. The talus below the cliffs shows that 
 among the strata are some of ironstone and conglomerate (with round milk-white quartz 
 pebbles), although these beds are concealed by the talus. From the hill-top similar hills 
 are seen to the north and south, all presenting their scarps to the east and dipping 
 gently to the west. From this point to Jericho the road is heavy white sand formed 
 from the waste of the Desert Sandstone én situ. ‘Len miles short of Jericho is a small 
 spring on the roadside, the water standing only a foot below the surface (even in the 
 terrible drought of 1885), and tasting strongly of lime. It is surrounded by calcareous 
 tufa.+ , 
 
 * The Aneroid altitudes taken on this journey are given, as being at least of value relative to one 
 another, although they are undoubtedly incorrect. The Railway Survey, for instance, makes the Barcaldine 
 Terminus 953 feet, and this locality must be at least a little higher than the crossing of the Alice, where our 
 Aneroid read 1,150 feet. 
 
 + Jericho, according to the Railway Survey, is 1,220 feet above the sea: the Aneroid made it 1,410 feet, 
 The readings between Dulbydilla and Jericho will have to be corrected accordingly 
 
516 
 
 Stewart’s Bore has been sunk for artesian water by the Government through 
 Desert Sandstone rocks, approximately in Lat. 24° 20’, Long. 146° 20’. 
 
 The bore is situated about midway between Tambo and Alpha Railway Station, 
 It ““was completed to the contract depth of 2,000 feet, unfortunately without tapping 
 overflowing water, and this is the first Government bore in which no overflowing artesian 
 water has been tapped:since the present system of boring was introduced in 1887. The 
 strata pierced have been clays, shales, conglomerates, and sandstones of the Desert 
 Sandstone or Upper Cretaceous Formation.’’* 
 
 This bore is interesting and unique. All the successful bores in the Western 
 District have obtained their supply of water from the Lower Cretaceous rocks. Itis quite 
 possible that if the bore had been continued to the base of the Desert Sandstone, water 
 would have been met with, but it is unlikely that it would have overflowed at the surface, 
 as the moisture with which the Desert Sandstone is generally saturated has abundant 
 facilities for escaping (as it frequently does) at the base of the formation, where it 
 comes in contact with the argillaceous shales of the Rolling Downs (Lower Cretaceous). 
 
 According to the Railway Survey the highest point on the divide between the 
 Barcoo and Belyando Rivers crossed by the Central Railway is 1,448 feet. The Desert 
 Sandstone extends past this to a few miles east of Pine Hill Station (1,158 feet—255 
 miles from Rockhampton), where it probably overlies the rocks of the Drummond Range 
 (Star Formation). 
 
 This same tableland is by far the largest fragment of the Desert Sandstone which 
 has escaped denudation, extending, as it does, from the heads of the Warrego to the 
 heads of the Flinders, a distance of three hundred and thirty-six miles, with a breadth, 
 on the line of the Central Railway, of seventy-two miles. Further north, where I 
 crossed it in January, 1882, between the Thomson and Cape Rivers, its breadth is one 
 hundred and twenty miles. Travelling from west to east,t a “jump up” of about 
 fifty feet near the head of Jirking Creek, brought us from the Rolling Downs Formation 
 to the top of the Desert Sandstone Tableland. The junction of the two formations is 
 unconformable. The base of the Desert Sandstone, as seen at the “jump up,” is highly 
 ferruginous, and apparently of volcanic (ashy) origin. The immediately succeeding 
 beds are of tough hardened sandstone, almost quartzite.in places. Pebbles of the latter 
 are scattered all over the Rolling Downs to the west. The tableland extends eastward 
 to a line between Manoa Creek and the Campaspe River, and is so flat that to the eye 
 it appears a dead level except where it is intersected by streams. Sections of the rock 
 are consequently very rare. Beef-coloured sandstones and thin plates of yellow sandy 
 ironstone were seen about eight miles below the upper crossing of Amelia Creek, The 
 divide between the Landsborough and Burdekin waters, although marked on the Colony 
 Map as a continuous mountain chain, is imperceptible. A great part of the tableland 
 is thickly timbered with rather stunted ironbark, bloodwood, box, and gum, and grassed 
 with Zriodia. Near the Campaspe mica schists are met with, but there is nothing to 
 show whether the Desert Sandstone rests unconformably on these, or is faulted against 
 them. The former is more probable. 
 
 The same tableland is crossed by the Northern Railway from the one hundred 
 and twenty-three-mile peg (say 1,100 feet above sea-level) to about two hundred and 
 twenty-four miles (say 1,169 feet). At one hundred and sixty-two miles yellow, 
 brown, and white sandstones are quarried for building material, which is employed, 
 
 * Report of the Hydraulic Engineer for Year ending 30th June, 1889. Brisbane : by Authority : 
 1889. 
 
 + See Reports on the Geological Features of part of the District to be traversed by the proposed 
 Transcontinental Railway. By R. L. Jack, Brisbane: by Authority ; 1885. 
 
517 
 
 e.g.. in the foundation course of the Cathedral at Townsville. The level of the 
 surface of the Desert Sandstone at Burra (one hundred and sixty-nine miles) is 
 1,817 feet. From Coalbrook Railway Station (one hundred and ninety-five miles 
 from Townsville—say 1,423 feet) I crossed the Desert Sandstone in January, 
 1888,* on a course of N. 29° W. for a distance of eighteen miles to the Flinders. 
 The country was flat and tame. Almost from the left bank of the Flinders the waters 
 drain through open marshy plains and lightly timbered forest country southward into 
 Bullock Creek, one of the feeders of Cooper’s Creek. The divide between the Gulf 
 waters and those of the Great Australian Bight is thus crossed imperceptibly, although 
 on the Colony Map it is denoted by shading indicative of a chain of mountains. The 
 Desert Sandstone is covered by a more recent deposit of weathered, and in part water - 
 arranged material derived from its waste, and cemented together with peroxide of iron 
 and carbonate of lime. The soil derived from the latter deposit, it may be noticed, 
 bears better grass than is usual in Desert Sandstone country. A good part of the 
 district is fair pastoral land, with frequent patches of blue grass and only rare clumps 
 of Triodia. On the left bank of the Flinders the Desert Sandstone, with a total 
 thickness of about twenty feet, rests unconformably on Rolling Downs strata, including 
 some coal-seams. The Desert Sandstone here consists of thin, almost flaggy, beds of 
 yellow and white siliceous material, sometimes gritty and occasionally pebbly, the 
 pebbles being invariably of white quartz. The bedding-planes and joints of the sand- 
 stone are frequently coated with films or layers, up to one-eighth of an inch in thickness, 
 of binoxide of manganese. 
 
 The thinning out of the sandstones of the great tableland is again well exemplified 
 on the head of the Flinders River,+ where I saw it in September, 1881. I may observe 
 that I started on this journey with a broken collar-bone, and was consequently unable 
 to do much climbing. The granite range dividing the Burdekin from the Flinders is 
 crossed by the Dalrymple and Hughenden Road, at an elevation of 3,040 feet (by 
 Aneroid), and is flanked by.a deposit of basaltic lava, disposed in nearly horizontal beds 
 and extending to Dalrymple on the east, and to Tatoo Camp, seven miles above Wongalee 
 Station, on the west. At Tatoo Camp a gully cuts through the lowest bed of basalt and 
 exposes about fifty feet of the underlying Desert Sandstone. The sandstone is white 
 or yellowish, with false-bedding, and with soft ferruginous portions, apt to weather 
 into caverns. The only fossils observed were some twig-impressions. Triodia at once 
 takes possession of the soil where the Desert Sandstone comes to the surface. It 
 occupies, however, at this place, only a narrow belt of country. The basalt occurs in 
 outlying table-mountains between Porcupine Creek and the Flinders, as far as Mount 
 Beckford, where it rests on the Desert Sandstone at an elevation (by Aneroid) of 
 1,800 feet. 
 
 The Section (Plate 45, fig. 1) shows the relation of the Desert Sandstone and 
 basalt between the Burdekin and the Flinders. 
 
 The Runs Map of Mitchell District shows about a score of little isolated table- 
 lands, which are outliers from the large tableland above described, and attest the former 
 extension of the Desert Sandstone to the west, although at slightly lower levels than 
 that of the base of the main tableland. The Desert Sandstone undoubtedly covered 
 the whole Mitchell District, and the present surface of the Rolling Downs over the 
 
 whole district is only a little lower than, that on which the Desert Sandstone was 
 deposited. 4 
 
 * Report by R. L. Jack., On Coal Discoveries on the Flinders. Brisbane: by Authority : 1888. 
 + See Transcontinental Railway Report. By R. L. Jack. 1885, © 
 
518 
 
 Outliers of Desert Sandstone were seen to the north of the Flinders, opposite 
 Telemon (forty miles west of Hughenden), while I was travelling over the Rolling 
 Downs in 1881. 
 
 In reporting on the Cape River Diggings in 1868, Mr. Daintree wrote as 
 follows :— 
 
 “The stratified rocks which rest uneomformably on the auriferous slates to the 
 south-west, and so cut off the extension of gold-mining in that direction, are those which 
 form that barren desolation, locally called the ‘ Desert,’ from which the eastern tribu- 
 taries of the Thomson and Flinders Rivers take their rise. 
 
 “The upper beds of this series are coarse friable sandstones, supported by thick- 
 bedded conglomerates, underlayed in turn by white clays and shales, with inter- 
 stratified layers of carbonaceous matter, but no true coal was observed. Where 
 these conglomerates are seen resting on the mica-slates, as’ is frequently the 
 case in the upper branches of Rankin’s Mistake Creek, the gullies have been 
 worked, and payable gold obtained where this conglomerate forms the bottom, and 
 its broken-up fragments, the ‘ wash-dirt’; but as no attempt has been made to sink 
 through the cement (though here very thin) the question of whether gold exists as a 
 product of denudation of the old schist rocks, at this early period in the world’s history, 
 yet remains uncertain. 
 
 “Conglomerates and sandstones of the same lithological character, and occupy- 
 ing the same relative position in regard to the auriferous slates, were tested practically 
 by the Geological Survey of Victoria, in the Bacchus Marsh District, without finding 
 the ‘colour’ of gold; here, however, is renewed encouragement to re-investigate the 
 matter, as the miners in Conglomerate Gully found water-worn gold attached to small 
 pieces of cement, together with free gold.’’* 
 
 In 1890 Mr. Rands made a discovery which will revolutionise our ideas of the 
 value of the fossil Glossopteris in determining the horizon of the rocks in which it is 
 found. The following quotation is from his Report on the Cape Gold Field + :— 
 
 “Following up Betts’ Creek, to within about a mile of Conglomerate Gully, high 
 banks of sandstone and shale are seen to the southern side of the creek. The sand- 
 stone at the base is fifteen feet thick. It is a coarse white sandstone, with layers of 
 quartz pebbles in it, like that generally met with in the Desert Sandstone rocks. Above 
 this there is a layer of shale, and then alternate white and brown mud rocks. Above 
 these is a bed of sandstone, and then a thin bed of shale full of Glossopteris leaves. 
 Above this again is sandstone. The height of the bank is forty feet. The beds are 
 almost horizontal. I fortunately had an opportunity of submitting these fossils to Mr, 
 R. Etheridge, junr., who pronounced them to be undoubtedly Glossopteris. From the 
 character of these beds, and also from the stratigraphical position of similar beds, seen 
 in the railway cuttings on the range beyond Pentland towards Hughenden, where they 
 certainly overlie the Rolling Downs Formation, I would pronounce them to be Desert 
 Sandstone. 
 
 “Tf this be the case, however, then the plant Glossopteris must have a much 
 longer range in time than has hitherto been suspected, as it was supposed to be confined 
 to the Paleozoic rocks, or at most to range as high as the Lotver Mesozoic. Mr. Etheridge 
 has determined the supposed Glossopteris of the Burrum Coal Field and of Stewart’s Creek, 
 near Rockhampton, to be a form of Teniopteris.} 
 
 
 
 * Report on the Cape River Diggings and the latest Mineral Discoveries in Northern Queensland. By 
 Richard Daintree. Brisbane: by Authority ; 1868. 
 + Brisbane: by Authority : 1891, p. 10. 
 
 + Phyllopteris, (R.E, June) . 
 
 
 
 
 
 
 
 
 
519 
 
 “At the mouth of Oxley Creek bold cliffs of white sandstone oceur which extend 
 away in an east-south-easterly direction. The cliffs here are about three hundred feet 
 in height. 
 
 “In the bed of White Mountain Creek, opposite the mouth of Oxley Creek, 
 there is a bed of brown shale in which the plant Oalamites * occurs in great numbers. 
 Above the shale the rock consists almost entirely of coarse white sandstone, with layers 
 of quartz pebbles, and also thin beds of shale and conglomerate. Oalamites occurs again 
 in aa iron-stained sandstone higher up the cliff. Near the junction with the schists 
 these beds are dipping S.W. at 25°, but further in they are horizontal. 
 
 “These beds extend away down to Betts’ Creek, crossing the railway line at the 
 range.. They can be seen as far as eye can reach from Mount Black and the range 
 behind Mount Black. 
 
 “ White Mountain Creek has cut a deep channel through the sandstone from 
 Oxley Creek to its junction with the Walker or Flinders River, a distance of about three 
 and a-half miles. 
 
 “ Following up Walker River, the stream has cut a somewhat narrow channel or 
 cafion, two hundred feet in depth, through the Desert Sandstone and the basalt which 
 here overlies it. The Desert Sandstone consists of a coarse, thick-bedded sandstone, 
 with layers of quartz pebbles, beds of conglomerate, and thin beds of shale. The sand- 
 stone shows false-bedding in parts. The overlying basalt is about 50 feet in thickness. 
 
 “ About two and a-half to three miles up the river from the junction of White 
 Mountain Creek, the Desert Sandstone is seen faulted against the schists by a fault 
 running east-south-east and dipping south-south-west. The schists and Desert 
 Sandstone are both covered with basalt. The Desert Saridstone is bent up near the 
 fault, and is dipping south-south-west. The section is well seen in the bank of the 
 river.” 
 
 Mr. Rands’ observations on this point seemed of so much importance that in July, 
 1891, I visited the scene of his discovery with the view of settling whether the beds in 
 which he found G@lossopteris really belonged to the Desert Sandstone. 
 
 About a mile south-west of the junction of Paddy’s Gully with Running Creek, 
 I struck Betts’ Creek, which I traversed for a little over a mile to its junction with 
 Conglomerate Gully. The latter I identified from the description on page 10 of Mr. 
 Rands’ Report on the Cape, of a section of sandstunes and shale. Iran up Betts’ Creek 
 for about a mile further, and then returning to where I had first struck the creek, rode 
 down the creek to the crossing of the old road and telegraph line from Capeville to 
 Hughenden. Nearly horizontal conglomerate sandstones and shales were met with on 
 both sides of Betts’ Creek for the greater part of the distance. I was not fortunate 
 enough to find the “thin bed of shale full of Glossopteris leaves” referred to by Mr. 
 Rands, although in several beds of shale [ could see indistinct and fragmentary plant- 
 remains, and the sandstones occasionally retained impressions of large limbs or trunks of 
 trees. 
 
 The sandstone rocks are traversed by the Northern Railway Line from the 1523- 
 mile peg (from Townsville) to the 215-mile peg. At the former they overlie the 
 auriferous schists of the Cape Gold Field, and at the latter they overlie the shales of the 
 Rolling Downs or Lower Cretaceous Formation, in both cases unconformably. On the 
 Flinders, as described elsewhere, they overlie the coal-bearing Lower Cretaceous rocks. 
 There can be no doubt of the continuity of the Desert Sandstone over this immense 
 area, and it must be accepted as an established fact that Glossopteris, which is abundant 
 
 
 
 —= 
 
 * Probably Hquisetum. (RE. Junr.) . 
 
520 
 
 in the Permo-Carboniferous Coal Measures, re-appears in the Desert Sandstone. As yet 
 its presence has not been detected in the Zeniopteris-bearing Burrum Beds, nor in the 
 Teniopteris-bearing Ipswich Beds, nor inthe Lower Cretaceous Rolling Downs Formation. 
 Whether its absence from these formations is simply due to imperfect collecting, or 
 whether the plant really migrated from the Australian Region after Permian times, to 
 re-appear at the close of Mesozoic times, there is no evidence toshow. It may any day be 
 found in the lower members of the Mesozoic Period. A long controversy was carried on as 
 to the age of the Glossopteris-bearing beds, the late Rev. W. B. Clarke and Mr. Daintree 
 insisting that the plant was Paleeozoic—a view which received confirmation when it was 
 found on the Bowen River, together with Productus, Spirifer, and other Paleozoic 
 fossils of the Lower or Marine Series.of the Bowen River Coal Field; while Pro- 
 fessor McCoy restricted the plant to the Mesozoic formations. It has been generally 
 understood that the question had been settled triumphantly in favour of Mr. Clarke’s 
 view, but we must now admit that Glossopteris also, as a genus, existed in Permo- 
 Carboniferous times, and survived till the close of the Mesozoic Period. Glossop- 
 teris occurs in India in Jurassic beds, and it may for some unknown reason have 
 migrated to that country during the period in which it has been missed from Australian 
 formations. 
 
 Mr. Rands’ discovery leaves no further room for doubt as to the correctness of 
 the observation of Mr. Norman Taylor, who refers to Glossopteris in the sandstone 
 tablelands between the Mitchell and the Walsh, as will be subsequently mentioned—an 
 observation which I was inclined to explain away by some theory of the Desert Sand- 
 stone of that region being a distinct formation from that in which Glossopteris was 
 found to occur. I believed that the section must be something like that seen on Oaky 
 Creek and the Normanby and Little Kennedy Rivers in the Cooktown District, where 
 the Desert Sandstone rests unconformably on the upturned edges of Glossopteris- 
 bearing strata. Mr. Taylor, naturally, considering the views accepted at the time 
 regarding the age of Glossopteris, mapped the tableland in question as Carboniferous ; 
 but there can no longer be any difficulty in recognising it as belonging to the Desert 
 Sandstone, of which it is evidently a denuded fragment. 
 
 Mount Nicholson, on the west side of the Cloncurry River, about four miles 
 north of the Township of Cloncurry, is a tableland which, as seen from any point of the 
 compass, shows unmistakably a horizontal capping of stratified rocks resting on older 
 rocks. I found (in September, 1881) the slopes to be of a decomposed gneissose rock, 
 and the top* had a thickness of twenty feet of coarse, gritty, siliceous sandstone, 
 occasionally pebbly (the pebbles mainly of white quartz), horizontally bedded. The 
 sandstone was “baked” throughout, and in parts might be fairly described as a quartzite. 
 
 Up the Cloncurry the “Soldier’s Cap” and two other small tablelands show 
 cappings of horizontal Desert Sandstone resting on slate. 
 
 Two outliers of horizontal Desert Sandstone rest on upturned slate and quartzite 
 rocks near the head of Cabbage-tree Creek, a tributary of the Leichhardt. 
 
 The late Mr. Richard Daintree refers + to the Desert Sandstone as extending from 
 Donor’s Hills on the north to the Dugald River on the south (left bank of Cloncurry 
 River). ‘Again, on the same parallel, between the Norman and Gilbert, two degrees 
 of longitude could be passed over without seeing any but the ‘ Desert Rocks’ exposed, 
 except in the deeper valleys.’’ The rocks here referred to come down to not very far 
 above the sea-level. 
 
 * About 1,200 feeb above the sea-level, but my Aneroid had become unreliable. ‘ 
 + General Report upon the Northern District. By Richard Daintree, Esquire, late Government 
 Geologist for Northern Queensland. Brisbane: by Authority : 1870. 
 
 
 
 
 
521 
 
 Mr. (now the Honble.) W. O. Hodgkinson, in his “ Diary of the North-Western 
 Fxpedition, 1876,”* refers to Desert Sandstone capping slates at the head of the 
 Templeton. 
 
 Mr. A. C. Gregory, in travelling down the Nicholson in August, 1856,+ noted 
 near the head of that river “ country consisting of steep sandstone ridges covered with 
 Triodia and a few stunted cuealypti,” leaving little doubt that the Desert Sandstone 
 fragments extend to the extreme western boundary of the Colony. In fact, Mr. Gregory, 
 who among Australian Explorers, stands conspicuous for accuracy and power of observa- 
 tion, had no hesitation in recognising the Desert Sandstone far to the west of these 
 limits. 
 
 On the divide between the Burdekin and the Lynd, in Lat. 18° 50'S., a low 
 tableland of ferruginous Desert Sandstone is seen on the north side of the Townsville 
 and Etheridge Road. The sandstone rests directly on granite. On the same road, near 
 Doughboy Creek, sixteen miles south-east of Grey’s Creek, are cliffs of about fifty feet 
 in height, of soft, red, ferruginous sandstones and conglomerates, the pebbles of the 
 latter bene mainly of the brown and yellow Devonian Sandstones. The cliffs are the 
 edge of a tableland of Desert Sandstone, which extends south-westward nearly to the 
 Broken River. Other fragments of the Desert Sandstone are seen to right and left of 
 the road a few miles west of the “ Continong” Gold Mine. 
 
 In his Report on the “Geology and Mineral Resources of the Upper Burdekin,” { 
 Mr. Maitland describes, as follows, certain stratified rocks in the valley of ine 
 Burdekin :— 
 
 “Throughout the district, at all elevations, there occur isolated fragments of 
 reddish-coloured sandstones and conglomerates, which are provisionally regarded as being 
 of Desert Sandstone age. Nowhere were they found to contain any Fossils, nor was there 
 any great thickness of them visible in one section. 
 
 “The first exposure of these rocks is met with in the country drained by the 
 heads of Oakey Creek, at an altitude of about 2,300 feet above the level of the sea. 
 Here the rock consists of an angular quartzose grit, which further south passes into a 
 brecciated conglomerate. 
 
 “Lower down the creek, near its junction with the Burdekin, a series of well- 
 nigh horizontal conglomerates and grits is crossed by the track from Kangaroo Hills 
 Station to Donnybrook ; a conspicuous escarpment of a higher member of the series 
 can be traced by the eye for a considerable distance east and west. 
 
 “Near the head of one of the branches of the Douglas River a similar series of 
 angular grits and conglomerates is seen to overlie the granite. The area occupied by 
 these rocks is small. 
 
 “The road from the crossing of the Burdekin, near Greenvale Station, to the 
 Valley of Lagoons, is flanked on its western side with tables of red sandstone, which 
 doubtless belong to the Desert Sandstone system. In the vicinity of the Valley of 
 Lagoons Station these rocks form well-marked escarpments, running up to the heads of 
 minor gullies, which empty themselves into the lagoons with which the eastern bank of 
 the Burdekin is studded. In one place these rocks are seen to consist of brecciated 
 conglomerates made up of large sub-angular fragments of quartz and mica-schist set in 
 a reddish-brown sandy matrix. These rest upon the upturned edges of the quartzites, 
 schists, &e. 
 
 * Brisbane: by Authority. 
 
 + Journals of Australian Explorations—by A. C. Gregory and F. T, Gregory. Brisbane: James 
 C. Beal, Government Printer : 1884, p. 169, 
 
 t Brisbane : by Authority : 1891, 
 
522 
 
 “ A creek entering the Burdekin from the west exposes in a cliff on its northern 
 bank a bed of conglomerate similar to that above described, resting upon schists, and 
 covered by a compact basalt sheet. 
 
 “The divide between the Herbert and Burdekin is capped by horizontal beds of 
 friable ferruginous sandstone, derived apparently from the denudation of granitic rocks; 
 these rest alternately upon acidic lavas and granite. 
 
 “Tn Blackwater Creek, a tributary of the Burdekin, what are taken to be 
 representatives of the Desert Sandstone make their appearance on either bank of the 
 river, and are seen to rest upon granite. From this section it appears that the Desert 
 Sandstone beds were laid down in the already denuded Burdekin Valley. 
 
 “Coarse ferruginous conglomerates or breccias, in the more immediate vicinity of 
 Wairuna Station, rest upon the vertical edges of the slates, &c’, which make up a large 
 portion of the neighbourhood. On the south side of the Burdekin, between Wairuna 
 and Lake Lucy, these Desert Sandstone rocks are well developed; they often form con- 
 spicuous cliffs, of no great height, which can be followed by the eye for some distance. 
 
 ‘The bridle-road from Wairuna to Lake Lucy crosses a tableland of ferruginous 
 sandstone for about four miles in a southerly direction. The southern face of this is 
 made up of a very red ferruginous grit, the material cementing the quartz grains being 
 an earthy hematite. 
 
 “From Oakhili Station to the summit of the Main Coast Range several exposures 
 of ferruginous sandstones are met with on either side of the road. These presenta 
 considerable lithological resemblance to those beds which cap the Main Range in the 
 vicinity of the Kangaroo Hills Tin Field. 
 
 ‘“‘The occurrence of fragments of these Cretaceous rocks throughout the whole 
 of the Upper Burdekin seems to indicate that tley originally occupied a very extensive 
 tract of country. That their thickness must have been considerable is evidenced by the 
 fact that their base occurs at all elevations above the sea-level. Taking the lowest 
 elevation (near the mouth of Oakey Creek) at which these beds are met with as being 
 1,300 feet, and the highest elevation of their base [?] as being 2,200 feet above the sea, 
 there cannot have been less than nine hundred feet of them; how much more it is at 
 present impossible to give any idea.” 
 
 A “ Geological Sketch Map of the Upper Gilbert” was published in 1869 by 
 Mr. Daintree. This map gives a very graphic idea of the relation of the Desert Sand- 
 stone to the older rocks, but as the topography of the map on which the geological lines 
 were laid down was very inaccurate, it must be regarded rather as a diagram than as a 
 delineation of the facts of the case. It shows correctly the Desert Sandstone resting 
 unconformably on older rocks, such as granite, porphyry, mica-schist, slate, &e., on the 
 summit of the Newcastle Range, forming the tableland between Gilberton and the 
 Woolgar, and extending in isolated denuded tables over the high lands intersected by 
 the Gilbert, Robertson, and Percy Rivers, and Agate, Cave, and other creeks. As, 
 however, I found, on travelling over the country in 1889, that many of Daintree’s 
 names have not passed into general use, and that owing to the inaccuracies of the map 
 on which he laid down his work his localities often could not be identified, I shall ” 
 content myself with recording some of the observations recently made by myself in this 
 region. 
 
 The Delaney River, a large tributary of the Etheridge, into which it empties 
 itself at Georgetown, splits up near its head into Delaney Creek, Goldsmith’s Creek, 
 Caledonian Creek, and others. These creeks rise on the edge of a tableland of Desert 
 Sandstone, denuded into numerous fragments partly covering the gneisses, schists, 
 slates, and granites which form the groundwork of the high lands between the Robertson 
 
 
 
 
 
523 
 
 and the Etheridge waters. Two miles west of the confluence of Goldsmith’s and 
 Caledonian Creeks a tableland, known as “Goldsmith’s Flat-top,’” rests on granite. A 
 similar tableland occurs a mile or so to the north. ‘The Castle” is a tableland 
 having an area of abouta quarter of an acre, three miles to the west of “ Goldsmith’s 
 Flat-top,’’ showmg a thickness of about thirty feet of white pebbly sandstone or 
 conglomerate, the pebbles being of quartz. It rests on granite, on the highest ground 
 in the neighbourhood. From this summit “ Mount Flat-top” and another Desert 
 Sandstone tableland can be seen about twelve miles to the west, near the head of 
 Western Creek, a tributary of the Gilbert. 
 
 About four miles north of Goldsmith’s Township a long tableland of Desert 
 Sandstone, on the high lands between Goldsmith’s Creek and the Sandy Etheridge, is 
 crossed by the direct road from Goldsmith’s to Townsville. 
 
 The broken fragments of the Desert Sandstone tableland on the divide between 
 the head of Goldsmith’s Creek and the Robertson River, rise to an elevation of about 
 2,200 feet above the sea, while the base of the sandstone rests, at 2,110 feet (by 
 Aneroid), on schists and slates. 
 
 On the Robertson waters, about two miles south of the divide between the 
 Robertson and Goldsmith’s Creek, a-lofty bluff of bedded trachyte lava rests directly on 
 a coarse volcanic ash, which passes in places into a conglomerate. Pl. 50, fig. 3, is a 
 section explanatory of the supposed structure of this region. The volcanic ash and 
 overlying bedded trachyte are probably contemporaneous with the altered ashes of the 
 Neweastle Range. Although the trachyte and ash have not been observed in the 
 district actually in contact with the Desert Sandstone, it is likely enough that it dates 
 from the earlier part of the same period. Between Mount Hogan and Gilberton, on 
 Chance Creek, a mass of coarse volcanic ash occurs, resting on slates and schists. The 
 alteration which the ash has undergone is greater than that of the Robertson and less 
 than that of the Newcastle Range, but I think it represents a contemporaneous deposit. 
 The section of the ash and trachyte is very much like some of those observed by Mr. 
 Maitland in the Mackay District, afterwards referred to. 
 
 Twenty-four miles south of the head of Caledonian Creek, the track from Gold- 
 smith’s to the Homeward Bound Mining Camp on the Percy River, after crossing the 
 Robertson and running up McCoy’s Creek to its source, goes through a gap on the 
 divide between the Robertson and Percy waters, fifteen miles north of the Homeward 
 Bound Camp. To east and west of the gap are cliffs of Desert Sandstone—white, 
 cross-bedded, siliceous, pebbly grits, the pebbles being of quartz and slate. Considering 
 that the sandstone rests directly on grey granite, the absence of granite pebbles (for 
 which I searched in vain) is very remarkable. I saw one agate pebble, and ferruginous 
 siliceous concretions very like those which form the matrix of the opal in the west. 
 The sandstone is in one bed about thirty feet thick. In other places a higher bed of ° 
 about the same thickness is seen. ‘The base of the sandstone (by Aneroid) is 2,135 feet 
 above the sea-level. 
 
 The track from Charleston, vid Tweedside, to the Homeward Bound Camp on 
 the Percy, about three miles north of the Percy, passes over a gap in granite country, 
 between two walls of conglomerate belonging to the Desert Sandstone series. The base 
 of the conglomerate is 2,240 feet above the sea. The same conglomerate is seen 
 capping. the hills between Agate Creek and the Percy, to right and left of the road. 
 Between the Percy and Mount Hogan Creek the Desert Sandstone is seen capping the 
 granite on the divide for six miles to right and left of the track. 
 
 Mount Nation, a conspicuous hill of Desert Sandstone, is on the right bank 
 of the Gilbert River, about two miles above Commissioner’s Hill. The hill consists of 
 
524 
 
 a single bed of coarse, gritty, sharp, white sandstone, about thirty feet thick, containing 
 imperfect plant-remains. The sandstone rests on slates and quartzites of the same age 
 as the goldfield at Commissioner’s Hill. 
 
 From Mount Nation, cliffs of the Desert Sandstone can be seen on the horizon to 
 the south and west, the edges of tablelands dividing the Gilbert from the Woolgar and 
 Norman. 
 
 In crossing the Newcastle Range, between Carpentaria Downs and the “ Stony 
 Etheridge,” the summit for about five miles is a tableland of soft yellow Desert Sand- 
 stone. It rests on a thickness of about five hundred feet of a clastic rock, resembling 
 a felspar porphyry, which in its turn lies on gneiss and mica schist. The Desert 
 Sandstone is nearly horizontal, but has a very slight dip to the west. 
 
 Some twenty-five miles further north, where the same range is crossed by the 
 telegraph line and road from Herberton to Georgetown, the road passes over a similar 
 clastic rock, on which, at an elevation of about 2,150 feet, by Aneroid, is an outlying 
 tableland of Desert Sandstone. 
 
 Down the right bank of the Etheridge River, below Georgetown, Mr. A. Gibb 
 Maitland, Assistant Geologist, noted in 1889, “at the head of Conglomerate Creek, a 
 tributary of Lane’s Creek, a tableland of Desert Sandstone, the beds forming which 
 lie horizontally. The rocks are very coarse-grained, guasi-vitreous grits and fine 
 conglomerates, the base of which is, by Aneroid, one hundred feet above the town of 
 Georgetown.”* The latter is by Aneroid measurement 1,200 feet above sea-level. The 
 sandstone rests on quartzites, shales, and diorites very much resembling the rocks 
 prevalent on Commissioner’s Hill, Gilberton. 
 
 Down the Gilbert River, below Crooked Creek, the Desert Sandstone occurs at 
 a level probably one thousand feet lower than at the heads of the river. At one point 
 seven miles down the river from Crooked Creek, and two miles to the west, a small 
 isolated hill had the following cliff-section :— 
 
 Feet. 
 Yellow, brown, and white sandstone ... whe an ae o abt) 
 Hard, brown, ferruginous, and siliceous sandstone, in part guasi-vitreous 2 
 Soft, fine-grained, white sandstone ... yes oa an os ae LO 
 Brown and yellow siliceous grit = va ey ve = ey ti 
 Granite débris, not waterworn ... ae at “ne Be 2 eet; 
 Totaly. i ie Ae ree : : ie se 
 
 These beds rested on granite, about one hundred and thirty feet above the level 
 of the Gilbert River. Smaller Desert Sandstone hills could be seen about three miles 
 to the south, and extending from north to north-east, at a distance of about five miles 
 from the river. 
 
 A mile west of O’Brien’s Station, on the Georgetown and Croydon Road, sand- 
 stones and conglomerates of the Desert Sandstone Series are seen on both sides of the 
 road, and nearly at the level of the road. The road and telegraph line, a little further 
 west, get upon a low Desert Sandstone tableland, over which they are carried as far as 
 the Gilbert River Telegraph Station. The road, after crossing the Gilbert River at the 
 telegraph station, traverses Desert Sandstone for five miles and a-half. Some porphyry 
 ridges are next crossed over, rising to a height of perhaps one hundred feet above the level 
 of the Desert Sandstone. Three miles further a red bluff, and.a mile further a white 
 bluff of Desert Sandstone, are seen on the south side of the road. After crossing the 
 Little River, the road rounds a cliff of Desert Sandstone on the south, and another is 
 
 
 
 * Report on the Lane’s Creek Diggings. Brisbane: by Authority: 1890, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
525 
 
 seen at some distance to the north. Four miles short of Flanagan’s or “The Springs” 
 Camp, the divide between the Gilbert and Norman waters is crossed. This watershed, 
 although marked on the Colony Map as the prolongation of the Gregory Range, is a 
 quite insignificant elevation, composed of gritty Desert Sandstone, resting on granite 
 and porphyry, at probably less than seven hundred feet above the sea-level.* 
 
 Opposite Flanagan’s, the eastmost camp on the Croydon Gold Field, are “The 
 Springs.’ These well out with a volume which supplies a five-head battery at the base 
 of a cliff of about thirty feet of Desert Sandstone, which rests on granite about one 
 hundred feet above the camp. This sandstone is plentifully charged with impressions of 
 marine Mollusca. 
 
 The same tableland extends for about three miles to the south-west to the 
 ‘* Alluvial Springs’’ (near Goldfield Homestead Area No. 120), and how much further I 
 do not know. The springs amply supply a vegetable garden below the cliffs, owned by 
 a Croydon Company. A little alluvial gold is found in gullies draining from the sand- 
 stone tablelands near the ‘ Alluvial Springs.” 
 
 About one mile north-east of the King of Croydon Claim, the ‘“ Richmond”’ auri- 
 ferous reef occurs in granite country, and its cap is covered by a horizontal cake of 
 Desert Sandstone, at a level of about one hundred feet above the surrounding flat 
 country. The lowest bed is a very coarse conglomerate, about twenty feet in thickness, 
 and above it is a thin bed of quwasi-vitrified sandstone with indistinct plant-remains. 
 
 On the divide between Belmore and Cork-tree Creeks, about two and a-half miles 
 east of Croydon Township, the “ Connaught Ranger’’ and another auriferous reef, in a 
 country rock of semi-vitreous quartz porphyry, are capped by a cake of Desert Sandstone 
 named Mount Angus, consisting of two beds, the upper ot quwasi-vitrified white 
 sandstone with plant-remains, and the lower of yellowish gritty sandstone with 
 molluscan fossils. 
 
 North of Belmore Creek, above the mouth of the Mountain Maid Creek, there 
 are three small outliers of Desert Sandstone. These, especially the two easternmost ones, 
 contain plentiful but imperfect impressions of jointed bamboo-like plants. I was informed 
 that ferns have been obtained from the westernmost of the three, and searched for them, 
 but without success. 
 
 The summit of the ridge between the Queen of Croydon Reef and the Pioneer 
 Machine on Belmore Creek is capped by sixty feet of horizontal white sandstone (De 
 Vis Hill). In this sandstone, which is in part gwas7-vitreous, I saw some impressions of 
 Pelecypoda, which, however, were not in sufficiently good order to be worth collecting, 
 and impressions of branches of trees up to four feet in length. 
 
 The True Blue Reef, in granite country, north of Croydon, is worked up to the 
 base of the Desert Sandstone. At the Prospecting Claim there are only a few feet of 
 sandstone on the cap of the reef, while on the “‘ Numbers,” to the south-east, the sand- 
 stone rapidly deepens. The diagram section (Pl. 45, fig. 2) from north-west to south- 
 east across the True Blue Hill shows the relation of the Desert Sandstone to the granite. 
 It will be observed that the beds of the former overlap. The uppermost bed is quasi- 
 vitreous, and contains twig-impressions and ferns, viz.—Didymosorus (?) gleichenoides, 
 Old. and Mor., var.t lreceived from Mr. Spencer, Manager of the Queensland National 
 Bank at Croydon, some handsome specimens of this fern, now in the Geological Survey 
 Museum. 
 
 
 
 * Geological Observations in the North of Queensland, 1886-7. By R. L. Jack. Brisbane: by 
 Authority : 1887. , 
 
 + R. Etheridge, Junr., Additions to the Fossil Flora of Eastern Australia. Proc, Linn. Soc. 
 N.S. Wales, iii. (2), Pl, 38, fig. 3. 
 
526 
 
 The beds beneath are of white gritty sandstone with a few quartz pebbles, which 
 have yielded several species of Pelecypoda, &e. 
 
 The upper level in the “ True Blue No. 2 South” Claim shows that the sandstone 
 is locally faulted against the granite as in the section (Plate 45, fig. 3). 
 
 A series of shafts sunk to the south-east of the hill in search of the True Blue 
 Reef, commencing below the level of the lowest bed of sandstone seen on the hill, shows 
 that a thickness of from thirty to sixty feet feet of white sand rarely consolidated to 
 sandstone, underlies the strata seen on the summit of the hill, and rests on granite. 
 But for the sections laid bare by these shafts the heavy sandy country south and east 
 ‘of the True Blue Hill, and connecting it with De Vis Hill to the north-east, would 
 certainly be taken as mere débris washed from the hill. Some of the Southern areas 
 therefore, already described as covered with saudy “débris of the Desert Sandstone 
 tablelands,’ may represent the formation actually cn situ. 
 
 By the Railway Survey Croydon is three hundred and sixty-one feet above the 
 sea-level, just on the edge of the sandy country. The base of the Desert Sandstone, 
 therefore, has come down from 2,240 feet at the heads of the Percy, to three hundred 
 and sixty feet at Croydon. 
 
 From a few miles north of Croydon to Normanton, the road passes over a dreary 
 expanse of low, level, sandy country, which falls indeed far cenit Normanton, although 
 the gradeis too gentle to be detected by the eye. In all probability the greater part of 
 this district is covered by Desert Sandst ne, although it is devoid of sections throwing 
 any direct light on its structure, or at least none were to be seen wheu I travelled over 
 it in December, 1889, the whole country being almostone sheet of water. The precisely 
 similar country to the east of Normanton is described by Daintree * as covered, over 
 two degrees of latitude, from the Norman to the Gilbert, by Desert Sandstone. 
 
 In a Report by Mr. A. Gibb Maitland, “On the Geological Features of the 
 Environs of Normanton,’ + the Desert Sandstone Rocks of that neighbourhood are 
 thus described :— 
 
 “Apart from the superficial deposits, the beds of the Desert Sandstone Series 
 occupy by far the greater portion of the surface of the district. Inthe absence of any 
 trustworthy data it is impossible to give any idea of their thickness. A variable 
 thickness of concretionary ferruginous sandstone, not unlike a conglomerate in appear- 
 ance, forms the upper portion of the series. Beneath this lie clayey sandstones, red, 
 brown, and even white in colour, which pass in places into rocks possessing all the 
 characters of true clays. In the well-sections seen within the municipal boundary, 
 these sandstones are associated with clay shales and true clay beds, often lenticular in 
 shape and of no great horizontal extent, and which in colour are generally yellowish- 
 white. A bore put down in 1885 by the Carpentaria Divisional Board at the junction 
 of Thompson and Woodward Streets, within the municipal boundary, shows ‘ironstone 
 rock,’ ‘mild rock,’ sandstone, and clay to a depth of two hundred and twenty-four feet. 
 The height of the surface of the bore is thirty-seven feet above high-water mark. It is 
 greatly to be regretted that no samples of the material passed through have been kept, 
 more particularly the ‘very hard rock’ met with when it was decided that boring opera- 
 tions should cease. From an examination of the record and from what is actually seen 
 in the well-sections, the whole thickness of rocks is provisionally classed with the Desert 
 Sandstone. It is, however, probable that what are described as ‘ clays’ are not all true 
 clays, but merely sandstones and shales containing a high percentage of argillaceous matter. 
 
 
 
 
 
 * General Report upon the Northern District. Brisbane: by Authority : 1870, 
 + Brisbane: by Authority : 1890. x 
 
 
 
 
 
 
 
—"v? a 
 
 527 
 
 “On the western side of the ridge upon which the Hospital now stands, a quarry 
 has been opened. The rock quarried is a very ferruginous fine-grained argillaceous 
 sandstone; but the percentage of clayey matter is not so high as in the beds more 
 immediately above. Beneath this, now covered by water, lies a bed of fairly porous 
 reddish sandstone, the thickness of which has as yet been undetermined. The escarp- 
 ment of these beds can be easily traced round to a point on the western bank of the 
 Norman, within six yards of the bank of the river. 
 
 “Similar sections are seen in a conspicuous cliff which can be traced along the 
 Cloncurry road as far as the Four-mile Creek, and also at intervals along the Burketown 
 Road, near Selection 72. 
 
 “ At the Red Bluff, twenty miles north-west of Normanton, and on the western 
 bank of the Norman River, a tableland of Desert Sandstone identical in physical 
 characters with that forming the rest of the district occurs. Its summit is sixteen feet 
 above high-water mark, and nowhere is the lower portion seen, being concealed beneath 
 superficial accumulations, which here attain a considerable thickness. 
 
 “A very thin capping of the concretionary sandstone of Desert Sandstone age 
 overlies the ‘ Rolling Downs’ formation, on a ridge about ninety feet above the sea, 
 at Magowra Station, between the Bynoe and Norman Rivers.” 
 
 The Stokes Range, to the north of Magowra, is a tableland of Desert Sand- 
 stone rising to ninety or a hundred feet above sea-level. The Reap Hook Range, further 
 to the south, is a similar Desert Sandstone tableland. The poverty in nomenclature 
 which applies the epithet of “range” to such elevations may be noticed in passing. 
 
 In the Cape York Peninsula the Desert Sandstone is well developed. It is most 
 conspicuous at Mount Mulligan, on the left bank of the Hodgkinson River, where it 
 rests unconformably on the vertical greywackes and shales of the Hodgkinson Gold 
 Field. As seen to the west of Weodville, the lowest bed is a coarse conglomerate, with 
 a grey matrix of granite débris. The pebbles uf this conglomerate are mostly of quartz 
 and quartzite, with a few of porphyry and granite. Some are of hardened greywacke 
 and a few of hardened shale. The conglomerate is about sixty feet in thickness, and 
 contains occasional partings of red shale or laminated mud. The next succeeding bed is 
 of red sandstone, and forms mural precipices one hundred and fifty feet high, without a 
 single practicable gap in a distance of ten or twelve miles. The Mount Mulligan 
 Plateau, a few years ago, was one of the strongholds of the Aboriginal population.* From 
 the summit, the J)esert Sandstone can be seen in isolated tablelands stretching far to the 
 west. Mount Mulligan is probably about 1,900 feet above the level of the sea, while 
 the greywackes and shales of the Hodgkinson Gold Field rise in the range between 
 Thornborough and Kingsborough, to an elevation of 2,530 feet. This range must have 
 formed part of the shore of the waters in which the Desert Sandstone was deposited. 
 The late Rev. J. E. Tenison Woods gives the thickness of the sandstone beds of Mount 
 Malligan as six hundred feet,+ which is obviously an over-estimate. 
 
 From the head of Limestone Creek, a tributary of the Mitchell, south of May- 
 town, I saw, in 1887, that some of the low hills south of the Mitchell were capped by 
 horizontal beds of stratified rock, probably the continuation of Mount Mulligan. This 
 is the place referred to by Mr. Norman Taylor, the Geologist who accompanied Hann’s 
 Expedition in 1872, who has kindly placed his notes at my disposal :— 
 
 “At Camp XVI.,on the Mitchell River, which was also Camp LXXVIII. on our 
 return journey, I found in the river-bed fragments and blocks of coal shales, with thin 
 
 
 
 
 
 
 
 * Report on the Hodgkinson Gold Field. By R. L. Jack. Brisbane: by Authority : 1884. 
 + The Hodgkinson Gold Field, Northern Queensland. Trans. R, Soc, Vict., 1881, xvii,, p. 1, 
 
528 
 
 seams of coal, and on searching carefully I discovered pieces of a whitish indurated 
 shale, containing indistinct plant-remains, and an undoubted fragment of Glossopteris. 
 (The shales are identical with some in the Blue Mountains of New South Wales, north 
 of Wallerawang, and again at Tallawang, north of Gulgong.) About a mile south of 
 this camp is a low table-topped rise, consisting of horizontal white and grey shales, 
 and a cherty-looking rock with fragments and stems of plants and traces of Glossopteris 
 tn situ. This rests on porphyry, hick forms a series of rocky hills two miles further 
 south, extending seven miles south-easterly to the foot of, and underlying, some high 
 table-topped Carboniferous ranges (composed of sandstones, grits, and conglomerates, 
 with silicified wood) in that direction. The Carboniferous range is about five hundred 
 feet above the river.’’* 
 
 I have always found it very difficult to reconcile Mr. Taylor’s observations with 
 my own ideas on lhe subject of the age of these sandstones. That the “ high table- 
 topped ranges” are denuded fragments of the Desert Sandstone I have no doubt 
 whatever. Mr. Taylor naturally, while it was the almost universal belief that the 
 presence of Glossopteris proved the formation in which it occurred to be Paleozoic, 
 mapped the tableland as. “Carboniferous,” and the ‘Carboniferous Range’’ still 
 figures on the Map of the Colony. Since, however, Mr. Rands has detected Glossop- 
 teris in beds belonging to the Desert Sandstone, and resting unconformably on the 
 Lower Cretaceous strata of the Rolling Downs, there need no longer be any difficulty 
 in admitting the Desert Sandstone age of Mr. Taylor’s tableland. 
 
 Mr. A. Gibb Maitland describes + the Carborough Range at the heads of the 
 Isaacs, as “composed of a series of conglomerates, grits, and sandstones, about five 
 hundred feet in thickness, which are arranged in a series of synclinal troughs, whose 
 longer axes run generally north-west to south-east. The base consists of a coarse, 
 somewhat felspathie grit, dipping at angles from 7° to 9° to S.W.W., the upper portion 
 being much finer in grain, and made up of a fairly fine-grained ferruginous sandstone. 
 Beneath these beds the upper or freshwater series of the Bowen River Beds is observable.” 
 The summit of the range is 1,750 feet above the level of the sea, and about seven 
 hundred feet above that of the surrounding country. 
 
 The Redcliff Range and its outlying fragment to the north, between the heads 
 of the Bowen River and Cerito Creek, consist of over eight hundred feet of rigidly 
 horizontal beds, mainly of a coarse grit of well-rounded grains of silica with a few 
 quartz and felstone pebbles. Some beds are more felspathic. The grit is white or 
 yellow, but often weathers with a reddish tinge. These tablelands rest unconformably 
 on the Upper or Freshwater Series of the Bowen River Coal Field.{ When I first saw 
 the Mount Leslie Sandstones in 1878 I doubted their identity with the Desert Sandstone, 
 but a much more extensive acquaintance with that formation has long since removed 
 the difficulties which I then saw. 
 
 Mr. Maitland,§ writing in 1889, observes that Mount Leslie is “made up of 
 sandstones, grits, and conglomerates similar to those forming the Carborough Range, of 
 which, physically, it is a continuation.” 
 
 Between the Sellheim Silver Mines and Mount Conway Station, the granite on 
 the divide between the Two-Mile and Percy Douglas Creeks is covered in places by 
 isolated table mountains, fragments of a once widespread tableland of horizontally 
 
 
 
 * Mr. Taylor’s MS. notes, penes me. 
 
 + Report on Geological Observations at the heads of the Isaacs, the Suttor, and the Bowen Rivers, 
 p. 4. Brisbane: by Authority : 1889. 
 
 + Report on the Bowen River Coal Field. By R. L. Jack. Brisbane: by Authority: 1879. 
 
 § Op. cit., p. 5. 
 
529 
 
 bedded Desert Sandstone. One of these, which I visited, showed, in the escarpment by 
 which it was bounded, fifty feet of yellow siliceous sandstone, somewhat ferruginous, on 
 fifty feet of white aluminous grit with quartz grains. Again, on the divide between the 
 Sellheim and Rosetta Creek, fragments of the Desert Sandstone tableland are seen on 
 either side of the road from the Silver Mines to Mount Conway, resting on syenite.* 
 
 “On the divide between St. Paul’s Creek and Cattle Creek, the granite is capped 
 with beds of Desert Sandstone, which is made up of beds of white sandstone with 
 layers of quartz pebbles, and beds of conglomerate made up chiefly of pebbles of 
 quartz. The Desert Sandstone forms bold cliffs which face the north, and it has 
 gradually thinned away by denudation towards the south. It extends about three miles 
 across in a north and south direction. Beyond this, granite shows again in the creeks 
 and gullies. The Desert Sandstone beds are nearly horizontal.’ + 
 
 In the neighbourhood of Cooktown the Desert Sandstone is seen under some of 
 its most interesting aspects, insomuch as it contains coal-seams, and is associated with 
 immense outbursts of volcanic activity. 
 
 On the north shore of the estuary of the Endeavour River, I saw, in 1879, the 
 lowest beds of the formation resting horizontally on five hundred feet or more of vertical 
 slates. A thick bed of conglomerate at the base was succeeded by about four feet of 
 grey shales, the uppermost eight inches of which were mixed with thin layers of coal.t 
 
 At the heads of Oakey Creek, the Desert Sandstone is seen resting horizontally 
 on the upturned edges of the Bowen River (Permo-Carboniferous) Coal Measures, which 
 in turn lie unconformably on older slates and quartzites. 
 
 In 1879 I wrote as follows § :— 
 
 “From the starting-point at Cooktown an extensive view is obtained to the north 
 and west, the valleys of the Endeavour and its tributaries forming a depressed fore- 
 ground, which has the effect of throwing into strong relief the contour of the mountains 
 beyond. No one can fail to be struck by the immense masses of horizontal sandstone 
 which cap the mountains in continuous tablelands at the heads of the Endeavour and ~ 
 Oakey, and in isolated fragments at Cunningham’s Range, Connor’s Knob, and Cape 
 Bedford. It must be obvious to the most superficial observer that the horizontal deposit 
 must have been continuous at no very distant date, even over the area where it is now 
 only represented by fragments standing alone on pinnacles of slate or granite, and that 
 the southern shores of the waters in which it was deposited were formed by the lofty 
 ranges from which the Annan, Normanby, and Laura Rivers take their rise. North of 
 this limit, or ancient shore, all the mountains which rise to the height of about eight 
 hundred feet above the level of the sea ‘catch’ (to use a graphic mining term) the even || 
 bottom of the sandstone, while from those which do not attain this altitude, as well as 
 from the valleys, the deposit has been entirely removed by denudation. 
 
 “With one notable exception, the sandstone, from the Byerstown Road northward 
 to the Morgan, rests upon a formation of nearly vertical strata of alternating slate, 
 quartzite, and greywacke. The edges of the slates and other upturned strata bear for 
 the most part north and south. The exception referred to occurs in the valley of Oakey 
 
 * Report by R. L. Jack on the Sellheim Silver Mines and Surrounding District. Brisbane: by 
 Authority : 1889. 
 
 + Report on the Cape River Gold Field, by William H. Rands, p.16. Brisbane: by Authority : 
 1891, 
 
 + Second Report by R. L. Jack on the Progress of the Search for Coal in the Cook District. 
 Brisbane : by Authority : 1879. ; 
 
 § Report on Explorations in Cape York Peninsula, 1879-80, By R. L. Jack, Brisbane ; by Authority ; 
 1881. 
 
 || Very uneven I haye since found it, 
 
 2K 
 
530 
 
 Creek, between the Palmerviile and Byerstown Roads. There the sandstone overlies, not 
 the slates, quartzites, &c., but a great thickness of strata containing Glossopteris 
 [Permo-Carboniferous or Bowen River Beds]. The beds of this formation dip at high 
 angles to the north-west wnder the horizontal sandstone [Desert Sandstone] of the 
 ‘ Brothers,’ which is therefore separated from them by a violent unconformability. As 
 a great thickness of the coal-bearing strata dips under the sandstone of the ‘Brothers’ 
 on the east side of that range, and does not reappear on the west side (where the sand- 
 stone rests immediately on slates), the coal-bearing strata must be bounded on the west 
 by a fault which passes beneath, and does not disturb the horizontal sandstones. 
 
 “The horizontal sandstone varies in texture from a coarse grit to a fine, hard, 
 eompact rock. The materials are for the most part siliceous, but occasionally felspathie. 
 Generally white or yellow, they sometimes have a faint red tinge from the presence of 
 peroxide of iron. Where much iron is present, nodules of fine hematite are frequently 
 met with. Pebbles of quartz, quartzite, slate, lydian stone, greywacke, and granite occur 
 near the base of the formation, forming a few beds of conglomerate. In the far north 
 of the Cape York Peninsula, as will be hereafter seen, the upper beds of the forma- 
 tion assume an entirely different aspect. There are very few shaley beds among the 
 sandstones. On the north side of the estuary of the Endeavour, however, some shales 
 are seen crowded with plant-débris. Indistinct plant-remains have also been met with 
 on Jane’s Tableland. Thin (quarter-inch) coal-seams occur on the north shore near 
 Cooktown, and in Temple Bay.” 
 
 The Morgan Tableland is a fragment of the Desert Sandstone, about four miles 
 across, and resting on upturned slates. 
 
 West of the Morgan Tableland is another large tableland of Desert Sandstone, 
 resting at an estimated elevation of four hundred feet above the sea-level, sometimes on 
 slates and greywackes, and occasionally oa granite or porphyry. Its northern edge 
 trends west-north-west, and is drained by the Starcke and Jeannie Rivers. A tributary 
 of the left bank of the Jeannie divides this tableland from another, though less extensive, 
 fragment extending towards Cape Melville. Cape Melville itself, as seen from the sea, 
 consists of apparently a thickness of three or four hundred feet of Desert Sandstone, 
 coming down to the sea-level and slightly undulating. Cape Bowen, to the south, shows 
 also a great thickness of Desert Sandstone, apparently quite horizontal, and resting on 
 slates (?) perhaps one hundred feet above sea-level. At Cape Flattery a great thickness 
 of gently undulating Desert Sandstone beds comes down to the sea in places, and in 
 others highly inclined schists are seen underlying the sandstone in the sea-cliffs. Here 
 the lower third or so of the formation is of brown sandstones and shales, and the upper 
 two-thirds of white sandstone. 
 
 At Cape Bedford, as seen from the sea, the Desert Sandstone forms a small 
 isolated tableland perched on slaty rocks, at apparently about four hundred feet above 
 the sea-level. 
 
 The tableland, whose eastern extremity at the heads of the Endeavour has already 
 been referred to, is reached by the Cooktown and Palmerville Road, a few miles east of the 
 Normanby River. Atits edge it is seen resting on nearly vertical slates and greywackes. 
 After making a “ jump-up” of two or three hundred feet, the road passes over horizontal 
 beds of white sandstone, for many miles, but on the left bank of the Normanby a 
 _mountain-mass of grey granite is seen, possibly of later date than the Desert Sandstone, 
 at least the absence of granite pebbles at the base. of the latter appears to favour that 
 view. After passing the Normanby the road, as far as Battle Camp, passes over, or 
 rather ploughs through, heavy, sandy, level country, the soil being probably all derived 
 from the waste of an underlying horizontal bed. At Battle Camp the road clears the 
 
 ni i 
 
5381 
 
 northern extremity of a “range’’ of hills (where the blacks made a determined stand 
 against the intrusion of white men on the first rush to the Palmer), and makes 
 more directly for the Palmer. The Battle Camp Range rises to about two hundred 
 feet above the general level of the tableland, and is composed of greenish-grey and 
 sometimes reddish sandstones. Mr. Norman Taylor, of the Geological Survey of 
 Victoria, who accompanied Hann’s Exploring Expedition in 1872, found in the Battle 
 Camp Range some fossils, which Mr. Robert Etheridge, F.R.S., described as “a Hinnites 
 hke H. lavetrix, and an Ostrealike O. Sowerbyi, Eth.” The discovery of two fossils not 
 specifically determinable, and of genera which have a wide range in time, does not count 
 for much, but the undoubtedly marine character of the fossils proves at least that this 
 portion of the Desert Sandstone was not of lacustrine, fluviatile, or aérial origin. Mr. 
 Taylor’s description of the locality is given (from his manuscript notes), as it may aid 
 in the re-discovery of the fossiliferous bed, which Mr. A. C. Macmillan has seen, but 
 which [ have searched for in vain on four different occasions :— 
 
 “ Ata point on the north-east side of an isolated table range (since named I 
 believe ‘ Battle Camp’) about four miles west of Camp 42, and close by a blacks’ corrob- 
 boree ground, I discovered, at the foot of the escarpment of horizontal sandstones, a very 
 hard siliceous greenish conglomerate, full of lydite and quartz, and, at its junction with 
 the overlying sandstones, numerous bivalves (Hinnites aud Ostrea). Above is a thick 
 series of greenish and reddish-brown, and also white fine grits and sandstones, with 
 concretionary ironstone bands. The sandstones contain a large quantity of silicified 
 wood, which, with the concretionary ironstone, lies scattered at the foot of the escarp- 
 ment.” 
 
 At the “ Kennedy Bend”’ (in “ Osmer No. 3” Block),* the river cuts through a 
 conglomerate (below the level of the base of the Battle Camp Range), containing 
 pebbles of conglomerate, quartzite, quartz, greywacke, slate, and a few of granite. 
 Higher beds of the series rise north of the Bend, to about three hundred feet above the 
 Kennedy. These are horizontal gritty sandstones, white and yellow in colour, with 
 much peroxide of iron, often segregating into concretionary masses. It may be 
 mentioned that these beds are seen to be penetrated by an intrusive mass of pink 
 felstone. 
 
 In 1879 I made two traverses across the western portion of the Desert Sandstone 
 Tableland, the first in a south-east direction to the Kennedy Bend, when returning from 
 the Coen Gold Field, and the second from the Bend, and keeping a few miles further to 
 the west, when starting out for Somerset with a Prospecting Party. 
 
 On the first course, a distance of thirty-five miles was travelled without seeing 
 anything but red sandy soil, with the exception of a slight ridge of ferruginous conglome- 
 rate, another of ferruginous sandstone, and some horizontal beds of white and yellow 
 gritty sandstone in a creek, while to the north-east the continuation of the low range of 
 higher beds seen at ‘the Bend was visible in the distance. It ended in a bluff of one 
 hundred feet of sandstone resting on granite. Our party had to beat about the bluff 
 for five miles before a place was found where the horses could get up. The sandstone 
 of the bluff was a very hard, coarse, ferruginous grit, with ironstone nodules and indis- 
 tinct plant-remains, 
 
 On the second course, we met with very much similar country, but the edge of the 
 tableland was found to present a thickness of at least five hundred feet of sandstone, 
 which we found difficult to descend from on to the underlying granite.+ It may 
 
 
 
 * See Two-mile Map Kennedy District, Sheet 12, 1889. 
 + Report on Explorations in Cape York Peninsula, 1879-80. By R. L. Jack. Brisbane: by 
 Authority : 1881, 
 
532 
 
 be mentioned that this part of the tableland is fair pastoral country, to which the term 
 of “ Desert” by no means applies. 
 
 The base of the tableland is here considerably higher than the ‘watershed of the 
 Cape York Peninsula crossed by us to the north-west. 
 
 The Railway from Cooktown to the Palmer (now open as far as the Laura) passes 
 to the south of the Battle Camp Range. After passing the Palmer Road Station (thirty- 
 one miles), and traversing granite country for a few miles (intrusive through the Desert 
 Sandstone, or forming a very uneven bottom, over which it was laid down), for six miles, 
 gritty, white, and brownish sandstones, with grey and dark shales, are seen in the rail- 
 way cutting, dipping at about 15° to the west. Similar strata continue to be seen in the 
 railway cuttings at least as far as forty-one miles and three-quarters, dipping on the 
 whole to the west. At forty-one miles sixty-two chains, I was informed by Mr. Webb, 
 that a two-inch coal seam was exposed by a man engaged in quarrying railway ballast, 
 but the water was so high that I was unable to see it. 
 
 A mile south-west of the thirty-nine miles sixty chains peg a branch of Welcome 
 Creek exposes some black shales with coaly streaks. Two miles south-east of this place 
 a shaft has been sunk in the bed of a gully below a waterfall, and on the banks and in 
 the bed of the gully were seen ten feet of grey gritty sandstone, with dark seams and 
 coaly streaks, overlying eight inches of black gritty sandstone, with coaly streaks. The 
 shaft was said to have been sunk eight feet on coal, but when I visited the place (in 
 February, 1887) the creek was, unfortunately, in flood, and I could only grapple for a 
 few samples. The coal had a specific gravity of 1°83, and on analysis gave the following 
 results :— 
 
 Per cent. 
 Moisture... ao be aa is pce a0 Tg OrZO 
 Volatile hy a hteer Os sick oe ae re er wee 80°42 
 Fixed carbon af ne on: ase wes A fs we 42°31 
 Ash ... oN uate ee a ee me ‘ie ae rae o02 
 
 Puckley’s Creek (which crosses the Railway near the thirty-seven mile peg), 
 about. two miles south of the railway, falls about fifty feet over a wall of granite, which 
 is capped by horizontal gritty sandstone. A mile above the fall, I saw grey sandstone 
 with bands of dark argillaceous sandstone containing imperfectly preserved plant- 
 remains, and little kernels of very good coal dipping down the creek (north) at about 
 7°. A mile further up, Mr. Webb pointed out a place where he informed me that 
 there was a seam of coal eight inches thick, then under water. About a mile further 
 up the stream the following section was seen dipping slightly down stream (north) :— 
 
 , Tt. in. 
 Gritty sandstone ess ge dite Ar ae Par </ we Oe 
 Goal t... sec “Ae A Se er ee Re EM Oak 
 Black sandstone x GA a * ae sh one ree, MOR AI) 
 Coal, said to be nd hes a Mahe a eo 
 
 Into the last-mentioned coal-seam I fant only sep. for Saree owing to the high 
 level of the water in the creek. The coal had a specific gravity of 1:55, and gave the 
 following results on analysis :— 
 
 Per cent. 
 Moisture... ane oes Be ee 5a ie ae UG 
 Volatile hydencacuoks oe a scl see 55 ve v. 20°96 
 Fixed carbon Pie a Ae sen ee ee te Se SUIeD 
 Ash . cae ae : we we A Res wae nn LOOLDe 
 
 It wili be aoe ann the two analyses that the proportion of ash is very high, 
 but it is quite possible that owing to the floods I may not have succeeded in procuring 
 good, or even fair samples. The posh however, resemble closely enough some which 
 
533 
 
 I saw in Mr. Webb’s possession, and at Cooktown, and which may be presumed to have 
 been collected under more favourable conditions than those obtained by me. Supposing 
 the mechanical impurities represented by the ash, and consisting, in the case of the 
 Welcome Seam, mainly of siliceous, and, in the case of Puckley’s Seam, mainly of 
 felspathic materials, to be lessened by about two-thirds, the coal would be valuable for 
 steaming purposes. As it is, the coals burn well enough, but their high percentage of 
 ash would interfere with their usefulness as fuel. 
 
 It is reported that in a well at Brown’s Station, about a mile north of the 
 northern escarpment of the Battle Camp Range, or Tableland, grey shales were met 
 with, which were supposed to belong to the coal-bearing series of Welcome and 
 Puckley’s Creeks. 
 
 On the left bank of the Little Laura, opposite Cobb’s Coach-stage, while halting 
 there on the journey from the Palmer, I saw an outcrop of horizontal grey clay-shales, 
 which I believed to be part of the Welcome Coal-bearing Series. 
 
 Regarding the age of these coal-bearing strata I could ascertain little or nothing, 
 having searched in vain for any recognisable fossils, and found only plentiful carbon- 
 aceous streaks representing decayed plant-remains. Mr. George Sweet, of Brunswick, 
 Melbourne, went to the Welcome Valley in June, 1889, expressly to make a similar search, 
 but was hardly more successful, although his collection included what could be recognised 
 as a fern and some reed-like plant-impressions. The strata are characterised by a great 
 paucity of fossils, which is itself a circumstance presenting a marked contrast to the 
 Permo-Carboniferous strata at Deep Creek, Oakey Creek, and the Little River. I 
 suspected from the first that the coal-bearing rocks of the Welcome Valley were part 
 and pareel of the Desert Sandstone, representing, like the coal-bearing rocks on the 
 north shore of the estuary of the Endeavour, a terrestrial or fresh-water phase of the 
 formation,* and this view has been abundantly confirmed by Mr. Maitland’s recent 
 investigations. 
 
 Mr. Maitland examined the coal-bearing deposits in the neighbourhood of Cook- 
 town in the end of 1890. His observations, which definitely settle the question of the 
 age of the deposits, are quoted below:— 
 
 “The beds of the Endeavour River, the Normanby River, and the Welcome 
 Valley have been examined and described by Mr. R. L. Jack in the years 1879 and 1887. 
 In the description of the latter, no definite conclusion as to the age of the Welcome 
 Valley Beds was arrived at. Subsequent examination shows them to be of Desert 
 Sandstone age. ‘ 
 
 “ Wherever examined they present very much the same lithological characters, 
 For the most part they consist of coarse sandstones, grits, and conglomerates. Many 
 of the sandstones in the higher portions of the series contain large quantities of hematite 
 in the form of irregular nodules. Fine-grained flaggy sandstones (with streaks of coal), 
 shales (some of a buff colour), and thin coals also occur, but they form a relatively 
 small portion of the series. A fine ashy sandstone, similar to the sandstone described 
 as occurring at the base of the Desert Sandstone in the Cape York Peninsula, near the 
 Lukin River, at Pera Head, north of the Archer River and Pisonia Island, one of the 
 Wellesley Group, off Point Parker, is to be seen at one portion of Battle Camp Range, 
 resting upon the sandstones and grits to be described below. Nowhere do these rocks 
 appear to have undergone much disturbance since they were formed. 
 
 “At Guppy’s Tableland, between Cape Bedford and Indian Head, the base of the 
 Desert Sandstone, which rests, with a violent unconformability, upon the upturned edges 
 
 
 
 * Geological Observations in the North of Queensland, 1886-7. By R. L. Jack. Brisbane: by 
 Authority : 1887. 
 
534 
 
 of the quirtzites, greywackes, and slates, is, by Aneroid, five hundred and sixty feet 
 above the high-water mark on the beach. The lowest bed consists of a coarse quartzose 
 conglomerate of seventy feet in thickness, succeeded by about fifty feet of fine-grained 
 Baber sandstones, with shales and thin coals, and in turn overlain by about three hundred 
 feet of coarse massive grits. 
 
 “ The following is a section in descending order :— 
 
 Ft. in. 
 Massive grits with coal streaks .. vis 300 0 
 Carbonaceous shale with thin sandstone paring 720 
 Coal (Guppy’s seam) 2 : Ors 
 Fine-grained sandstone with ai laces 6 O 
 Big sandy shale with coal streaks 3 10 
 Sandstone ... oP ses es 2 0 
 Shale... 0 6-8 
 Sandstone 0 10° 
 Dark shale with ont streaks i OSG 
 Fine grained sandstone (with an irecalar hase) end thin Nab 6-8 0 
 Fine grained flaggy sandstone with thin lenticular beds of sandy 
 shale... si o a ee see wes re ec lOLZ eC 
 Quartzose conglomerate ... a ee Le 8/080 
 
 ““Guppy’s coal-seam has been eoneal up, on no fresh light is thrown upon the 
 section. There is no underclay or ‘seat earth’ beneath the weal A sample of this 
 seam, collected by myself, yielded on analysis :— 
 
 
 
 Moisture... aa ohn sh ae ane ae gp CABS 
 Volatile A yarosuepens Af str ane ane =e ae any | LBRAG 
 Fixed carbon aa ates oe - As ae a ayn TASB 
 Ash eee eee eee eee eee eee eee eee eee aoe 9°65 
 
 100:00 
 
 The specific gravity is 1:66. The ash is of a yellow colour. 
 
 “None of the beds in the section at Guppy’s Tableland have yielded any fossils 
 with the exception of a few plant-remains, rootlets and fragments of leaves, from some of 
 the carbonaceous shales. Fragments of coal are not uncommon in the upper grit. 
 
 “The section exposed at Indian Head is similar to that at Guppy’s Tableland, with 
 the exception that the total thickness of strata is not so great, there being only about 
 three hundred feet. The base lies at an altitude of about eight hundred feet above 
 high-water mark. The lower and upper grits are continuous from Guppy’s Tableland, 
 but they are separated by a smaller thickness of flaggy sandstones and very sandy 
 shales. A seam of coal is said to occur among these beds, doubtless a continuation of 
 that seen in Guppy’s Tableland. 
 
 “From this point westwards, the next outlier of sandstone is at Mount 
 Fantastic ; this consists of about one hundred feet of sandstone, with neither shales nor 
 coal. 
 
 “The tableland between Mount Fantastic and Connor’s Knob is of sandstone, as 
 is also Connor’s Knob. 
 
 “In examining the cliffs to the north of the Endeavour, near its head, I saw 
 nothing of any of the shales, the whole section appearing to be coarse massive sand- 
 stones. 
 
 ‘The hills in the neighbourhood of Brannighan’s Bluff, in Isabella Creek, are 
 reported to contain a thin seam of coal. 
 
 “Crossing the divide into the waters of the Normanby, the Desert Sandstone 
 Beds are found to be represented by sandstones and grits without any of the intervening 
 
535 
 
 shales. The base, near the railway, is at an altitude of four hundred feet above the 
 sea-level. In the distance intervening between Indian Head and the Normanby the 
 coal-bearing shales have disappeared. The shales make their appearance, however, in a 
 small synclinal trough seen in the railway cuttings near the thirty-seven-mile peg, at an 
 altitude of about four hundred and thirty feet above sea-level, or two hundred feet 
 below the horizon of those at Indian Head. At the eastern end of the section, at the 
 thirty-six-mile peg, the Desert Sandstone Beds rest presumably upon granite, which is 
 seen 7 situ two hundred yards distant to the southwards. A ridge of massive quartzite 
 is seen to rise from beneath the sandstones at the thirty-seven-mile peg. 
 
 “A cutting to the east of Battle Camp Creek exposes a conglomerate, with 
 pebbles of greywacke and quartzite, resting unconformably upon the massive quartzite 
 mentioned above. The conglomerate is covered with four feet six inches of black shale, 
 and that again by sandstone, the whole series dipping at angles varying from 5 to 
 7 degrees to the east. Buff-coloured sandstones are seen to lie beneath those at the 
 thirty-seven and a-quarter-mile peg. 
 
 “A cutting at the 37{-mile peg shows nothing but very false-bedded sandstones 
 of a reddish-white hue, with a few ‘ false dykes ’—7.e., fissures which have subsequently 
 been filled in with sandy matter. Beneath this false-bedded sandstone lies three feet of 
 shale, which dips at 5 degrees to the west. This rests on a continuation of the 
 sandstone seen at the 372-mile. 
 
 “Dipping at 3 to 5 degrees to the north is a bed of black shale, at the 38-mile. 
 At the 38}-mile this is underlain by greyish sandstone with ironstone nodules. The 
 hills on either side of the line are made up of nearly horizontally bedded rocks. 
 
 “Coarse grit, conglomerate, and a thin bed of shale are seen in the cutting at 
 the 383-mile. Some of the coarser grits and conglomerates contain kernels of shale. 
 On the south side of the line, near the 39-mile peg, granite rises from beneath the 
 grits. 
 
 “About a mile and a-half south of the 40-mile peg a bed of carbonaceous 
 shale with coal streaks, crowded with reed-like plants, too fragmentary for determina- 
 tion, is laid bare in one of the branches of Welcome Creek. The shale has a dip of 
 5 degrees to the west-south-west; it rests upon a bed of fine-grained sandstone of a 
 greenish hue. A shaft has been sunk upon the shales, but apparently abandoned a long 
 time previously.* A traverse from this point to the foot of the highest point in the 
 district—a conspicuous hill two miles to the south—shows nothing else but weli-nigh 
 horizontal sandstones. The sandstone capping the summit of the hill is very fine- 
 grained; its mural face contains many small caves, which have apparently served as 
 hiding-places for the natives. As viewed from the summit, the whole of the Welcome 
 Valley appeared to be made up of similar bedded rocks. 
 
 “ Wine-grained yellowish sandstone, with a low dip to the west, is laid bare at 
 the 40$-mile peg. 
 
 “The Battle Camp Range lies to the north of the line at this point. It is 
 composed of alternations of grits and sandstones, disposed with a gentle dip to the 
 south-east: one bed was found to contain annelid tracks (?). The summit, 870 feet above 
 sea-level, is made up of a fine ashy (?) sandstone, which rests apparently conformably 
 upon the other rocks. This ashy (?) sandstone only attains a thickness of about forty 
 feet, and is not continuous over a larger area. In its lithological characters it agrees 
 with those occurring further north in the Cape York Peninsula. I searched in vain for 
 fossils, annelid tracks (?) being all I could discover. (It was from the northern face of this 
 
 
 
 * See p. 532, 
 
536 
 
 range that Mr. Norman Taylor, the Geologist attached to Hann’s Expedition in the 
 year 1872, discovered Hinnites and Ostrea.) From the summit, as far as the eye could 
 reach, nothing but horizontally bedded rocks could be seen. 
 
 “A little distance east of the 41}-mile peg a quarry has been opened for ballast 
 on a horizontal sandstone of the usual type. A similar sandstone is seen in a cutting 
 between the 433 and the 43$ mile pegs. 
 
 “ Another ballast quarry has been opened to the south of the line—the 443-mile, 
 and distant about one hundred and fifty yards; the sandstone is fine in grain and of a 
 white colour. 
 
 ‘* Reddish-yellow, fine-grained sandstone dips to the east at angles varying from 
 5 to 10 degrees in the vicinity of the 44¢-mile peg. 
 
 ‘“‘A conspicuous escarpment of coarse gritty sandstone trends east and west, 
 distant about two hundred yards to the south of the 474-mile peg; a similar cliff— 
 probably a continuation—oceurs about half-a-mile to the south-east of the 49-mile peg. 
 
 “Tn the vicinity of the 553-mile, within two hundred yards of the line, on the 
 south, a series of fossils were collected from a bed of fairly coarse grit which occupies 
 the greater portion of the neighbourhood. The fossils, which resemble very closely 
 those occurring in the Desert Sandstone of Croydon, consist of Maccoyella (?), internal 
 casts of Rhynchonella, and others which I have not yet been able to determine.* 
 
 “From this point to the railway terminus at the Laura River, nothing but 
 sandstones of the usual type occupy the country on both sides of the line. 
 
 “Five miles up the Laura from the railway crossing, the following section is 
 seen, in descending order, in a cliff in the river :— 
 
 Tt. in. 
 Grits with pebbles me aes . 810 
 Shale... oH hg anh see ae 
 Coal ... ae oie Aad vee die 
 Shale ... ne 5 . 0 3 
 Grey sandstone rr Suis te ne wal a ORD 
 Sandy shale... = sis “5 Pes At o02L0 
 Fine-grained sandstone ... aa am a atk = eee 
 _  Bluish sandy shale Sr a 1 9 
 Coal ... Ae ene 0 5 
 Sandy shale... ave Cm 
 Sandstone 3h ee 0 0 
 
 “The whole of the beds lie etna In tie machen ower is an absence of 
 underclay or seat-earth heneath the coal. 
 
 - “ An instructive section is to be seen in Puckley or Sandy Creek. The altitude 
 of Mount Ruby Station is, by Aneroid, 420 feet above sea-level. A traverse from this 
 point to the divide between Leichhardt and Puckley Creeks showed coarse grits, lying 
 horizontally upon granite, at 1,000 feet above sea-level. The summit of the divide is 
 1,250 feet, thus giving a thickness of two hundred and fifty feet of sedimentary rocks at 
 the head of Leichhardt Creek. When, however, the waters of Puckley Creek are 
 followed down, it is found that the thickness of the sedimentary beds has increased to 
 five hundred al twenty feet. 
 
 ‘From the summit to 850 feet the whole of the noah consist of coarse grits and 
 
 conglomerates. At 380 feet below the summit, or 870 fect above sea-level, two seams 
 of coal are seen to be interstratified with the grits. A section in the bank of the creek 
 shows the lower seam of coal to be nine inches in thickness, three inches of the base 
 of which is crowded with quartz granules ‘to such an extent as to make it an 
 
 
 
 * This locality, by the Railway Survey, is about 466 feet above sea-level. 
 
537 
 open question whether the rock should be called coal or merely a carbonaceous grit. 
 Above this nine-inch seam lies a bed of grit two inches thick, and this is covered by 
 
 another coal seam of four inches. A sample of the coal from the upper portion of the 
 nine-inch seam was taken and submitted to analysis, with the following result :— 
 
 
 
 Moisture... oAS aa ee ot eh AD Hs ste Otaes 
 Volatile hydrocarbons... exe se aes aoe sa veo Ls 
 Fixed carbon ms ai ise Be be a6 ac we ©=89°84 
 Ash ... eee Ae =: a re se ee <6 nee 8020 
 
 100°00 
 
 The specific gravity is 151. The ash is grey in colour. 
 
 “A little distance west-north-west from the outcrop in the creek a shaft had 
 been sunk through sandstone, to a depth unknown to my informant, with the object of 
 meeting the coal. The shaft had been abandoned some time, and I was unable to descend. 
 
 ‘In the section described above there is an absence of underclay or seat-earth. 
 The coal rests directly upon coarse grit. It would appear as though the coal had been 
 formed in such a position as would allow of the access of sandy matter. The high 
 percentage of ash, as well as the gritty character of the base, gives credence to this view. 
 
 “ Following the windings of the creek for a mile or two down its course, sections 
 show nothing but fine-grained argillaceous and micaceous sandstones, with nodules of 
 ironstone and small pellets of coal. The beds roll about a good deal, but their dip 
 never measured more than from 5-7 degrees northwards. They rest upon a coarse sand- 
 stone described * as occurring at the spot where Puckley Creek falls over a wali of 
 granite 50 feet high. From this point to the railway the country is occupied by granite 
 of the usual type. 
 
 “ About a mile below the Railway Bridge a bed of coarse sandstone dips at a low 
 angle down the creek; it is seen to rest upon granite. 
 
 “Tt will be seen from the altitudes given that the Welcome Valley beds occupy a 
 position below those at the head of Puckley Creek. 
 
 ‘“‘ For the purpose of comparison, the analyses made of the Desert Sandstone 
 coals have been thrown into a tabular form. 
 
 ‘The description of the localities from which the coals analysed by Mr. R. L. 
 Jack were obtained need not be repeated—it will be found by referring to the Report 
 on ‘ Geological Observations in the North of Queensland’ already quoted. 
 
 ‘ ANALYSES OF THE CRETACEOUS CoALS OF THE COOKTOWN DISTRICT. 
 
 
 
 
 
 —— 1 2 3 4 
 Moisture ... as af, ia os 8°25 716 0°33 2°32 
 Volatile hydrocarbons... bi ah 30°42 20°96 30°13 15°20 
 Fixed carbon wie wes va ae 42°3] 35°35 39°34 72°83 
 Ash... ae AG oA ee 19°02 36°53 30°20 9°65 
 Specific gravity ... vee see sa 1°83 1°55 151 1°66 
 
 
 
 
 
 “1. Locality.—About three miles south of the 4-mile peg, Cooktown Railway; analysed by R. L. 
 Jack. 
 
 “2. Locality—About four miles up the Valley of Puckley Creek, above the Railway crossing ; 
 analysed by R. L. Jack. 
 
 “3. Locality.—Near the head of Puckley Creek; analysed by A. Gibb Maitland. 
 
 “4. Locality—Guppy’s Tableland, North Shore; analysed by A. Gibb Maitland. 
 
 
 
 * “ Geological Observations in the North of Queensland.” R.J. Jack. Brisbane: by Authority. 
 
538 
 
 “ After entering the valley of Welcome Creek, it will be seen that the thickness 
 of the Desert Sandstone beds increases somewhat rapidly to the westwards. At the 
 36-mile peg their base is, from the Railway Survey, 348 feet above sea-level. Between 
 this point and the Laura Terminus, which is 269 feet in height, the country is occupied 
 by one continuous series of sedimentary rocks, disposed in a series of scarcely 
 perceptible undulations, but with a gradual dip westwards. 
 
 “The total thickness of strata at the head of Puckley Creek is five hundred and 
 twenty feet; between the base of these and the top of the grits seen below the Puckley 
 Creek Bridge, 350 feet above sea-level, there is room for not less than five hundred feet 
 of rock. The sandstones of the Battle Camp Range, which rise to a height of 500 feet 
 above the beds at the 86-mile peg, are probably the. representatives of the beds which 
 occupied this gap. 
 
 “The Welcome Valley beds—by which term is meant the whole of the series of 
 rocks between the 36-mile and the Laura terminus—thus occupy a position below those 
 described as occurring at the head of Puckley Creek, and also below those of the Battle 
 Camp Range. It would be rash to venture upon an estimate of the thickness of the 
 beds of the Welcome Valley, for there has been no evidence brought forward to throw 
 any light upon this point. 
 
 “The minimum thickness of Desert Sandstone lying above the 36-mile peg, 
 where the Welcome Valley beds are first seen, is not less than one thousand feet—more 
 than double that occurring in the Endeavour waters. 
 
 “ Another point which the examination of this district has brought out is the 
 existence of a ridge running approximately parallel with the Normanby River north 
 and south. To the west of this ridge was a valley or hollow in which the Welcome 
 Valley beds were deposited. Where the western boundary of this hollow existed it 
 would be premature, with the meagre evidence before us, to state. To the southwards, 
 however, near the head of the Laura River in the Palmer River waters, the Railway 
 Survey gives the altitude of the base of the Desert Sandstone as being 1,100 feet above 
 sea-level. 
 
 “A circumstance worthy of note is the entire absence of an ‘ underclay’ or 
 ‘seat-earth’ from any of the Cretaceous coals of this district which have yet been 
 described. The coals either rest directly on grit or very sandy shale, and one of the 
 coals—that from Puckley Creek—has its base crowded with quartz grains. Some of 
 the shales contain very thin lamin of coal, which are not continuous for any great 
 distance. These peculiarities are due to the conditions under which the coals were 
 formed.” 
 
 In the Valley of the Little Kennedy, one of the heads of the Kennedy River, 
 highly inclined slates are seen on the left wall of the valley, capped by horizontally 
 bedded conglomerates and coarse gritty sandstones, forming a portion of the tableland 
 which has already been partly described. On the right wall of the valley the slates rise 
 to a much greater elevation than on the left, and must have formed a portion of the 
 shore of the waters in which the Desert Sandstone was deposited. The floor of the 
 valley shows Permo-Carboniferous rocks (including coal-seams) let in by two north and 
 south faults between the two masses of slate. The Permo-Carboniferoas rocks, as well as 
 the older slates, must have been covered unconformably by the Desert Sandstone.* 
 
 On the Road from Cooktown to Palmervillé, about four miles short of- the 
 latter, the base of the Desert Sandstone forming this extensive tableland is again seen 
 resting on vertical slates and a thick limestone bed. The Desert Sandstone here presents 
 
 
 
 * Report by R.L.J. on the Little River Coal Field, near Cooktown. Brisbane: by Authority : 1882. 
 
 
 
539 
 
 a precipitous escarpment of about four hundred feet in height, and consists mainly of 
 two beds—the upper of red sandstone, with a white band in the middle; and the lower 
 of a coarse conglomerate containing pebbles of quartz, gneiss, and granite in a matrix 
 of sharp white sand. The same escarpment can be traced eastward to near the head 
 of the Palmer, forming the right wall of the valley. The surface of the tabcland on the 
 Road from Cooktown to Maytown (on the top of the cliff overlooking the latter) is 
 given by Mr. Surveyor White as 1,500 feet, while Maytown is 800 feet. Mount Hann 
 and the “High Mountain” between the escarpment and the Palmer River rise 
 respectively to 2,250 and 2,300 feet, and must have stood up as islands in the Desert 
 Sandstone waters. 
 
 Mount Daintree, about ten miles west of Palmerville, is an outlier of the Desert 
 Sandstone, resting on gneiss, and forms a tableland of about ten acres in extent, 
 bounded by sheer cliffs, two or three hundred feet®in height, which can only be scaled in 
 one place. On this tableland the timber is stunted and the grass (Zriodia) is totally 
 different from that on the surrounding land. The cliff is composed of thick-bedded red 
 and white siliceous sandstone. One fine-grained white laminated bed is full of plant- 
 remains, which, however, are quite undistinguishable, though somewhat reed-like in 
 general appearance. This bed is probably identical with the “white band” above 
 referred to as occurring in the middle of the upper bed seen on the Palmerville and 
 Cooktown road. 
 
 From Mount Daintree I obtained (in 1887) a good view of the surrounding 
 country. Escarpments of Desert Sandstone extended along the north wall of the valley 
 of the Palmer, at distances varying from three to twelve miles, almost without 
 interruption, from a point bearing N.N.W. of the mountain to beyond the Maytown and 
 Cooktown roads. Subtending an angle from N.N.W to S.W. of Mount Daintree, the 
 whole of the country, as far as the eye could reach, was low and nearly level. (This 
 is the position assigned by Mr. Norman Taylor toa “Carboniferous Range’’ in the 
 Map attached to the account of Hann’s Northern Expedition.) About ten miles 
 south-south-west of Mount Daintree, high escarpments of horizontal strata were visible, 
 probably further outliers of the Desert Sandstone.* 
 
 In a Map of the Squatting Runs down the Palmer furnished to the Lands 
 Department by Messrs. White and Embly, the words ‘“ Desert Sandstone” are 
 written across the back of ‘“ Meron Downs” Block on the left bank of the Palmer, and 
 across the centre of ‘‘Strathleven No. IV.” Block on the right bank of the same river 
 (opposite its junction with the Mitchell). I have not seen these localities, but as I 
 know Mr. White to be a trustworthy observer, I regard the information as reliable, 
 especially as it agrees with Daintree’s observations on the Lower Gilbert. 
 
 Mr. James V. Mulligan, after leaving Palmerville on a prospecting trip, keeping 
 round the south-western end of the Main Desert Sandstone tableland, had to cross 
 another small table-land between the Palmer and Fahey Creek.f 
 
 Much of the alluvial gold of the Palmer Gold Field has been derived from the 
 immediate neighbourhood of the ‘“‘ Conglomerate’’ or Desert Sandstone tableland, and 
 in positions where it is impossible to ascribe its presence to the degradation of local 
 reefs. As there is no evidence of any submergence of this district beneath the sea 
 between Permo-Carboniferous and Cretaceous times, it is probable that the area covered 
 by the Desert Sandstone was a land surface for animmensely greater period prior to the 
 deposition than it has been since the elevation of the Desert Sandstone, and the uneven 
 
 
 
 * Report of the Government Geologist, in Annual Report of the Department of Mines for 1887. 
 + Report on Expedition in lav of Gold, &c., in the Palmer District by Mulligan and Party. 
 Brisbane : by Authority : 1876, 
 
540 
 
 bottom on which the Desert Sandstone has been deposited corroborates this view. Now, 
 if we admit that what was a land surface from Permian to Cretaceous times still lies 
 beneath the Desert Sandstone, we may confidently expect to find beneath it numerous 
 ancient watercourses, in which the débris from a very much larger area of auriferous 
 rocks than has been exposed since the denudation of the Sandstone must have been 
 “sluiced’’ again and again, so that the gold may be in “ leads” in a highly concentrated 
 form. I began to insist upon this view in 1836, and it is satisfactory to note that since 
 then payable gold has been obtained in consolidated drifts or “ cements” between the 
 base of the Desert Sandstone and the surface of the slates to the north of the Palmer. 
 
 Mr. Daintree, in 1872, expressed the opinion* that ‘‘ the very nature of its [the 
 Desert Sandstone’s] deposition seems to preclude the idea that gold will be found in 
 paying quantities, except where direct local abrasion of a rich auriferous veinstone has 
 furnished the supply. It is, indeed, doubtful if any marine or extensive lacustrine beds, 
 except on their shingle margins, have produced, or are ever likely to produce, remunera- 
 tive workings of free gold, for the simple reason that the majority of the sediments of 
 which they are composed are derived from formations the greater part of which were 
 non-auriferous.” My own conviction is that in the Palmer district deep leads, containing 
 an amount of gold which will dwarf into insignificance the four or five million pounds 
 worth already obtained from the field, will yet be found beneath, if not in, the Desert 
 Sandstone. Where an old land surface composed of auriferous rocks is covered over by 
 a newer deposit, it is likely that the deep leads thus preserved from denudation will 
 prove rich in gold. It matters nothing whether the covering be of basalt or sandstone. 
 
 The same remarks as to the presence of alluvial gold beneath the Desert Sand- 
 stone apply to many other fields inthe Colony. At the Upper Gilbert, at Croydon, 
 at the Cape, at the Hodgkinson, at the Starcke, and at Cania, the bulk of the alluvial 
 gold has been obtained from localities from which the Desert Sandstone has.been 
 recently denuded. In fact, when one thinks of it, the places where alluvial gold has 
 been found in conspicuously large quantities are just the places where these conditions 
 prevail, and not the places where the local reefs are richest. I have seen some 
 suggestive instances on the Palmer where rich gold has been obtained from gullies 
 within the whole drainage area of which there was no reef whatever. This may seem 
 a bold assertion, but the country was dry, the grass had been recently burnt, and every 
 bed of shale and sandstone in the drainage area was laid bare. Again, north of Tambo, 
 alluvial gold (I believe in small quantities) has been found in Windeyer Creek and 
 guilies which rise in the Desert Sandstone and flow over the underlying Rolling Downs 
 rocks. As the latter certainly contain no auriferous reefs, the probability is that the 
 gold was derived from ‘“‘leads” beneath the Desert Sandstone. 
 
 On our northward course to Cape York in 1879-80, we first struck the Desert 
 Sandstone between the Lukin and Kendall rivers, in about. Long. 143° EH. The sand- 
 stone ai its eastern escarpment had a thickness of about fifty feet, and was about 200 
 feet above the level of the plain. It was ferruginous and very hard, and appeared to 
 be partly composed of fine volcanic dust. It contained little pebbles of quartz and 
 larger pebbles of slate and quartzite. A granite mountain attaining a higher elevation 
 than the sandstone lay between it and the Lukin River. It is very probable that the 
 base of the Desert Sandstone rises gradually from near the sea-level on the Lower 
 Norman and Gilbert (where Daintree observed it) to the higher level near the junction 
 of the Palmer and Mitchell, where it is marked on the Plan of “ Strathleven No. IV.” 
 Squatting Block, where paleozoic rocks rise from beneath it. It would thus have 
 
 
 
 * Q.I.G.S., xxviii, p. 278, 
 
 
 
541 
 
 a gentle dip to the coast of the Gulf of Carpentaria. Its eastern escarpment, in ail 
 probability, from “Strathleven No. IV.” Block, keeps nearly the meridian of 148° E. 
 as far north as the divide between the Lukin and the Kendall. 
 
 Between the South Coen and the Peach River, our course took us over a con- 
 siderable area of the Desert Sandstone, presenting a steep escarpment to the east, which 
 I named the Geikie Range. The sandstone lies on granite. The Geikie Range is cut 
 through by the Peach. Our course, however, lay among the mountains (at a much higher 
 elevation) to the cast, so that we only saw this portion of the Geikie Range or tableland. 
 I may say, in passing, that on this portion of our journey we had a good deal of skirmishing 
 with the natives, who managed to kill the horse I was riding by aspear-thrust just behind 
 the saddle, and to wound the horse which carried another member of the party, so that 
 the acquisition of geological information was not altogether unattended with difficulty. 
 
 Between Canoe Creek and the Pascoe, outliers of the Desert Sandstone rest on 
 the tops of granite hills, while on the western or left bank of the Pascoe the 
 escarpment which prolongs the Geikie Range to the north continues in an unbroken 
 line. Granite mountains (the Janet Range) rise to the east of Canoe Creek to a height 
 of 1,245 feet. Far to the west (the eastern escarpment of the tableland forming the 
 watershed between the Batavia—Gulf waters—and the Pacific waters at the heads of 
 the Pascoe), a second escarpment marks the eastern limit of a higher bed of the Desert 
 Sandstone. This, which I named the Wilkinson Range, is now included in “ Merkunga”’ 
 and “ Merkunga South” Squatting Blocks. The greater part of the Desert Sandstone 
 country between Latitudes 12° and 16° S. is now taken up on pastoral leases (except 
 within the nominally “settled district’ extending thirty miles from the coast on both 
 sides of the peninsula, and in which the terms are less easy), so that the term “ Desert” 
 cannot apply to it. 
 
 Near the mouth of Canoe Creek we found the Desert Sandstone oecupying both 
 sides of the creek. Where this creek joins the Pascoe we built a canoe, or dug-out, by 
 which we crossed the flooded river. This must be about fifteen miles above the spot 
 where in 1848 the gentle and unfortunate Explorer Kennedy left the remainder of his 
 party when he set out on foot, accompanied only by his blackboy “ Jacky-Jacky,” to 
 meet his fate at the “ Escape Inlet,’ within sight of the ship which was to bring him 
 relief. The hills at Fair Cape were doubtless the last objects that met the eyes of his 
 companions as one by one they sickened and died, while waiting for the relief which 
 was to come too late for all but two of the number.* 
 
 North of the Pascoe we ascended to the top of a high escarpment of Desert 
 Sandstone (to which I gave the name of the Sir William Thompson Range). This 
 tableland extends from the valley of the Pascoe in Long. 143° 3’ H., and Lat. 12° 40'S., 
 north-north-eastward to the 12th parallel, and presents a steep escarpment to the 
 Pacific, and a long gradual slope towards the Gulf. The bed of sandstone of which the 
 tableland is composed is about five hundred feet in thickness,and is reddish and cemented 
 with iron oxide. <A lower shelf which crops out from beneath it is of yellow and white 
 sandstone, occasionally containing a few pebbles. The tableland and the lower shelf 
 decompose into soils which have a world-wide difference, the former being clotted with 
 good grass, and well timbered with stringy-bark, bloodwood, Pandanus, and Xanthorrhea, 
 while the latter was mainly covered with thickets of heath, and, as far as grass was con- 
 cerned, was a veritable desert. The lower beds of the shelf abut to the east against 
 serrated mountains rising to 2,342 feet, which I named the Carron Range, in commemora- 
 tion of the tragic circumstances connected with Dr. Carron’s stay when Kennedy left him 
 
 
 
 
 
 
 
 * Narrative of the Voyage of H.M.S. ‘‘ Rattlesnake.” By John McGillivray, F.R.G.S. Vol. i. 
 London, 1852. 
 
542 
 
 to set out on his last forlorn expedition. About Lat. 12° 30’ S. we saw the base beds of 
 the Desert Sandstone resting on granite. At the south-west corner of Temple Bay we 
 descended for about two hundred feet over the edges of the lower shelf of Desert 
 Sandstone to the porphyry on which it rests. The Desert. Sandstone comes down to 
 the sea-level at Temple Bay. At Bolt Head, in Temple Bay, thirty feet of horizontal 
 reddish sandstone lay unconformably on a blue limestone, at least a hundred feet in 
 thickness, and dipping at 45° to the east. 
 
 Further north the “ Remarkable Red Cliff” of the Admiralty Charts showed two 
 coal-seams, each a quarter of an inch in thickness, in the midst of red sandstone. 
 
 As far north as Camisade Creek the thick upper bed of sandstone forming the Sir 
 William Thompson Range and the lower shelf continued to present the same features, 
 the top of the eastern scarp of the former, although only a few miles from the Pacific, 
 being the watershed of the Peninsula. Camisade Creek and Bay, it may be mentioned, 
 were so named from the circumstance that here we had further trouble with blacks, 
 who this time, in the middle of the night, threw, among others, a spear which went 
 clean through the deltoid muscle on the right side of my neck. 
 
 An uncharted island, close to the coast, at a point bearing 8. 26° W. from the 
 south-east end of Fern Island, is of horizontal Desert Sandstone. At this point and 
 at the mouth of Iienderson Creek the red sandstone is highly ferruginous and has a 
 pisolitic structure. There is evidently a very gentle dip in the sandstones northward 
 from the Carron Range, so that: although the dip is almost imperceptible we gradually 
 pass over higher beds. 
 
 Among the intricacies of the swamps between the Escape Inlets and the Jardine 
 River we found the sandstone to be brown and ferruginous, with a pisolitic structure. 
 
 Both sides of the Albany Pass are composed of nearly horizontal beds of sand- 
 stone. Similar beds of sandstone are seen in Mount Adolphus Island to the north. 
 Towards Cape York slates rise from beneath the sandstone. At Thursday and 
 adjacent islands slaty rocks rise to a considerable altitude, but the Desert Sandstone is 
 seen in numerous headlands at the level of the sea. 
 
 About a mile west of Mount Morgan, near Rockhampton, is a mass— 
 apparently about a hundred and fifty feet in thickness—of horizontally bedded 
 Desert Sandstone. It rests, at this point, apparently on a mass of diabasic dolerite,* 
 but in other places it may be seen lying on the upturned edges of quartzite and 
 greywacke strata of Permo-Carboniferous age (like the Gympie beds) similar in 
 character to those of the “country” round Mount Morgan. The base of the Desert 
 Sandstone is a mass of fine volcanic dust, while the upper beds are coarsely gritty, and 
 for the most part siliceous, varying from white to brown and red. I should judge the 
 base of the formation to be about one hundred feet lower than the summit of 
 Mount Morgan, or one thousand one hundred and twenty-five feet above the sea. 
 The grit and conglomerate beds at the base of the Desert Sandstone in this district 
 contain, as in the Palmer District, gold, apparently inpa yable quantities. (Mount 
 Victoria. ) 
 
 Standing on the sandstone cliffs, so as to look eastward past the south side of 
 Mount Morgan, the observer can descry, across the valley of the Dee, the familiar 
 contour of horizontally bedded sandstone cliffs stretching from north to south over the 
 divide between the waters of the Dee and Gavial Creek. As nearly as can be judged 
 by the eye they are on the same level as the cliffs on the opposite side of the valley, and 
 
 
 
 
 
 * See Notes on a Collection of Rocks and Minerals from Mount Morgan. By C. 8S. Wilkinson, 
 T. W. Edgeworth David, and William Anderson. Records of the Geological Survey of N.S.W. Vol. ii., 
 Part'3, 1891. 
 
 
 
 
 
543 
 
 there can be no doubt that the valley has been carved out of a once continuous cake of 
 sandstone. In this valley the hot spring which gave rise to the auriferous deposit of 
 Mount Morgan subsequently broke out, as will be seen in a succeeding chapter. 
 
 In deseribing the Cania Gold Field * Mr. Rands writes :— 
 
 “A very conspicuous feature of the neighbourhood is the two long and lofty 
 lines of sandstone cliffs, which at the Cania Diggings are some six or more miles apart ; 
 but further down the creek, six or seven miles towards Cania Station, they approach one 
 another, forming high precipices on either side of the creek, and leaving only a narrow 
 gorge through which the road to the station passes, 
 
 “The cliff on the left-hand side, going down the creek, is perpendicular and 
 almost continuous for over twelve miles, and is never much more than a mile distant 
 from the Three Moon Creek. About two miles from the Township, where it must be at 
 least three hundred and fifty feet high, it has the appearance of the walls and battle- 
 ments of an old castle, giving to the hill the name of the “ Castle Mountain.” The cliff 
 on thé opposite or right-hand side of the creek is only perpendicular for short distances 
 here and there, and generally presents more of a sloping face. 
 
 “These cliffs consist of a white gritty sandstone, in parts stained red or brown 
 with oxide of iron. Every few feet, or even oftener, there are layers of a coarse grit, 
 or bands of rounded pebbles of white quartz, varying in size from one-quarter to three 
 inches in diameter. These bands serve to show the original stratification of the mass, 
 which is overlying the older rocks unconformably, dipping 5 degrees to S., 15 degrees 
 E. False-bedding in this sandstone is very frequent. The sandstone is very cavernous; 
 the face of the cliff has weathered, and where there has been least cohesion between 
 the particles of sand large caverns have been formed. 
 
 “These cliffs, standing perpendicularly, as they do, two or three hundred feet 
 high, and opposite to one another, bear witness to the great amount of denudation 
 which has taken place, for the whole country round about must have been formerly 
 overlaid by this formation ; its nonvaonteliy points to the fact that there has been but 
 little disturbance since its Aenpeean?? 
 
 Mr. Rands estimates the altitude of the base of the Desert Sandstone in this 
 locality roughly at 1,400 or 1,500 feet. 
 
 In Mr. Rands’ Report on the Albert and Logan District,+ he writes of the 
 Desert Sandstone as follows :— 
 
 “This formation, which at one time covered the greater part of Queensland, is 
 met with towards the heads of Nerang Creek, near Mr. Nixon’s selectiéns. It forms 
 the summit of the ranges between Mudgeeraba and Nerang Creek, and between Nixon’s 
 Creek and Back Creek. 
 
 “The thickness of this deposit is about one hundred and fifty feet, some distance 
 down the ranges; and increases to three or four hundred feet towards the heads 
 of the creeks. It stands out in bold perpendicular cliffs, full of small hollows or 
 eaves. At its base the deposit is a conglomerate, composed of rounded pebbles and 
 boulders of basalt, similar to that met with in the neighbourhood. Some of these 
 boulders are over 15 inches in diameter. Higher up, the rock consists of granular 
 siliceous sandstone, with thin layers of coarse quartz pebbles. 
 
 “The formation here certainly appears to be an ordinary sedimentary deposit, 
 and not of volcanic origin, as suggested by the Rev. J. E. Tenison Woods in a paper 
 read lately before the Royal Society of New South Wales.” 
 
 
 
 * Report on the Goldtields of Raglan, Calliope, Milton (Norton), and Cania, &. By William H., 
 Rands. Brisbane: by Authority : 1885. 
 + Brisbane: by Authority : 1889. 
 
544 
 
 The sandstone overlies part of the mass of basalt “ which is found capping nearly 
 all the higher ground of the district right away from the plains of the Darling Downs, 
 near Laidley, Grandchester, Ipswich, Waterford, Mount Tambourine, on the dividing 
 ranges between the Logan, Albert, and Coomera Rivers, and Nerang, Mudgeeraba, 
 Talleebudgera, and Curambin Creeks.* It is also met with at Burleigh Heads, Cor- 
 rumbin Heads, Point Danger, and on the Macpherson Range.” Mr. Rands informs 
 me that the base of the Desert Sandstone in this locality must be at least one hundred 
 and fifty feet above the sea. 
 
 In the Gympie District Mr. Rands describes the Desert Sandstone as follows :— 
 
 “This is a coarse-grained silicious sandstone, or freestone, which overlies the 
 Gympie Beds [Permo-Carboniferous] in various places. The rock is made up of coarse 
 granules of quartz. It lies horizontally, but nearly everywhere exhibits ‘false-bedding’ ; 
 the true bedding of the rock can be detected by thin layers of coarse pebbles of quartz. 
 A large outlier of this sandstone can be traced from Eel Creek, crossing the Mary near 
 the Fisherman’s Bend, where it forms high banks to the river. It has been quarrted as 
 a building stone near Eel Creek, on Mr. Dan. Henry’s Selection, No. 882, and it has 
 ‘been used in several of the principal buildings in the town. Outliers of this stone also 
 occur a few miles north of Gympie, near the Maryborough and Gympie Railway 
 Line.” + Mr. Rands believes the base of the Desert Sandstone to be here one hundred 
 and fifty feet above the sea-level. 
 
 Mr. Daintree, in 1872,+ referred to certain beds which “ crop out at the township 
 of Maryborough, and have been used by the Corporation as quarries for road-metal,’’ 
 and gave a list of fossils therefrom, as determined by Mr. Robert Etheridge, F.R.S. 
 These beds Mr. Daintree regarded as the upper portion of the Burrum Coal Measures, 
 and occupying “a position between the Gordon Downs and Flinders River series.” 
 More recent and extensive collections of fossils do not at all bear out this view, the fossils 
 on the contrary bearing a very close correspondence with those of the Desert Sandstone 
 at Croydon. Probably Mr. Daintree made only a hasty collection of fossils, as he does 
 not even give a description of the strata. 
 
 Mr. Rands has within the last few years carefully mapped out the beds and 
 
 shown their relation to the underlying Burrum Coal Measures. In his “ Report on the 
 - Burrum Coal Field,’”’§ he says, “The Maryborough Beds have been quarried about one 
 mile west-north-west of the Railway Station by the Corporation for road-metal, and by 
 the Government two miles further out in the same direction for railway ballast. The 
 
 rock quarried is a fine-grained, light brown or grey sandstone. These beds contain 
 numerous shells. 
 
 “At the Corporation quarry the strata consist of light-coloured, fine-grained ~ 
 
 sandstones, dipping 12° to N. 35° E. 
 “ Abouta mile and a-half further along the Gayndah Road, and close to the 
 Mary River, about half a miie from what is known as the Copenhagen Bend of the river, 
 
 is the first of the Government Quarries. The dip is about 7° E. The rocks showing 
 are :— 
 
 Ft, in, 
 Broken sandstone che. a 56 oo) 
 Grey, fine-grained sandstone (fossiliferous) : ae ee 
 Band of laminated sandstone wee OO 
 
 
 
 * T, for one, rejoice that the sentimental feeling which leads to the retention of unpronounceable 
 native names, for the most part conveying no meaning, and which, I believe, in some cases, will not bear 
 translation, is not universal. R.L.J. 
 
 + Report on Gympie Gold Field, By William H. Rands. Brisbane: by Authority ; 1889. 
 
 $Q.J.G.S., vol. xxviii., p. 288. § Brisbane: by Authority ; 1886, 
 
 
 
 
 
 
 
 
 
545 
 
 Le} 
 
 woOrFroworRoOononoanaonws 
 
 mBOoWMWOs 
 
 Grey sandstone (fossiliferous) 
 Band of laminated sandstone 
 Brown sandstone 
 
 Brown shaley sandstone 
 Greyish-brown sandstone (fosdilit=roun) 
 
 Fine laminated grey shale 
 
 Grey sandstone (fossiliferous) 
 
 Shaley band sit 
 
 Grey sandstone (foemliferous) 
 
 Black shale 
 
 Hard dark-grey leminated sandstone (fossiliferous) 
 Shale aes 
 
 Grey sandstone (fostiliferous) 
 
 Laminated argillaceous sandstone ... 
 
 Dark-grey sandstone ... 
 
 i 
 ome NwWKRO OK WOOD 
 
 | 
 
 41 
 
 “ A quarter of a mile further up, exposed in another quarry, dip 7-8° 
 are :— 
 
 Zo 
 
 35° E., 
 
 ~ 
 
 SSL) Se) SE 
 
 Brown sandstone with band of carbonaceous shale 
 Black carbonaceous arenaceous shales (fossiliferous) 
 Soft yellow sandstone 
 
 Shale and soft carbonaceous sandstone : mh te a 
 Coarse gritty sandstone oe aa a ee pas at nie 
 
 (ese) Mo 0} Ker ORK o ret 
 
 33 3 
 “ Just a couple of hundred yards on the Maryborough side of the Copenhagen 
 Bend, in a quarry, are showing thirty feet of grey sandstone, containing the ordinary 
 fossils met with in these beds, and also numerous casts of Belemnites.* Below this is a 
 thin bed of carbonaceous sandstone, and below this again fifty feet of brown and grey 
 sandstones (fossiliferous), dip 9° N. 35° E. Just in the centre of the bend, in a small 
 gully cut into the steep bank of the river, are exposed :— 
 
 Ft. in. 
 
 Horizontal sandstone, consisting of small quartz crystals cemented 
 together ... He ae bas he ee re fee ROAD 
 Soft argillaceous sandstone... ere 7 ae +e oa ay) EN 
 Soft yellow sandstone or ‘ai Boe ee a A, 
 Grey shale and nodular perbagnccae sandstone. a axe pe UU 
 Black shales with bands of brown and grey sandstone... ee yy BA AE 
 57 0 
 
 “These beds, it will be noticed, dip in the same direction, and have about the same 
 angle of inclination as the coal-bearing beds of Saltwater Creek and the Burrum River ; 
 and as they are not seen again beyond this point, it is possible that there is a fault 
 between them and the Burrum Series. Similar sandstones, too, with the characteristic 
 fossils of the Maryborough Beds, are met with in the Isis River, about a quarter of a 
 mile south-west of the Maryborough and Bundaberg Road, witha dip of from 30° to 
 45° to H. 40° N. These beds, which overlie the coal strata, can be traced for about 
 
 a’mile up a gully running into the Isis about half a mile higher up, but are not met with 
 in the river again. 
 
 * See Note under Belemnites, p. 574. 
 21 
 
546 
 
 “T met with sandstone, belonging to the same series, containing the Cretaceous 
 fossils Avicula alata, Leda elongata, and Nucula, &e., &c., about thirty-two miles 
 north-west of Bundaberg, and about ten miles south of Rosedale Station. Their dip was 
 uncertain, but they were evidently overlying the [Burrum] Coal Measures Series, which 
 is exposed about two miles south, in Littabella Creek, dipping 12° to the N.E.” 
 
 Mr. Rands writes me under date 16th September, 1889:—‘ I have come to the 
 conclusion, after another examination, that the Maryborough Beds have been brought 
 into their present position by a fault, and that they are unconformable with the Burrum 
 Series, occupying some local hollow, as shown in the section.” (Plate 46, fig. 3.) 
 
 Professor Ralph Tate, of Adelaide, after a careful study of the Organic Remains of 
 the Cretaceous rocks of South Australia, records his opinion that the Maryborough 
 Beds (Queensland) are of Cretaceous age.* . 
 
 In a Report on the “ Geological Features and Mineral Resources of the Mackay 
 District” + Mr. Maitland describes as follows certain “rocks probably the equivalent 
 of the Desert Sandstone Series” :— 
 
 “The rocks mapped as being the equivalents of the Desert Sandstone Series are 
 classed with them more on account of their analogy to rocks of that age in widely 
 separated localities than any stratigraphical or paleontological evidence collected would 
 warrant. Nowhere are they seen to rest upon any rocks the relative age of which has 
 been satisfactorily made out, and all that can be at present said of them is that they 
 overlie unconformably all the other rocks of the district, save upon those referred to 
 Post-Tertiary age. 
 
 “The strata consist of a series of trachytic lavas and subaqueous ashes, seen at 
 several localities in the country to the north of the Pioneer, and about four hundred 
 and fifty feet of sedimentary rocks, occurring in the cliffs forming the Cape Hills- 
 borough tableland, and an isolated fragment of coarse conglomerate near Cape 
 Palmerston. 
 
 “The lavas and ashes will be dealt with first, asin all probability they were 
 formed inthe early days of the history of this period. 
 
 “One of the most conspicuous examples of the lavas is to be found at Mount 
 Mandarana, better known as the Black Gin’s Leap, close to the Bowen Road, about 
 
 twelve miles north-west of Mackay, where it forms a broad table-like mass, rising to a © 
 
 height of 650 feet, by corrected Aneroid, above the level of the road. The rock of 
 which the Leap is made up is lithologically a trachyte, and may be generally described, 
 when examined with a lens, or the unaided eye, as consisting of a light-coloured porous 
 matrix, in which crystals of sanidine and minute crystals of what appear to be horn- 
 blende are embedded. It is seen (Plate 46, fig. 1) to rest upon black shales, at a 
 point in a gully flowing from the north-west corner of the mountain three hundred feet 
 above the road. At the junction of the two, the shales for a few inches are slightly 
 hardened. The lower portion of the sheet is made up of rudely hexagonal curved 
 columns, the outward curvature being northwards. The structure of certain parts of 
 this rock would seem to imply that in reality it is a succession of lava-flows of variable 
 thickness ; the estimated thickness of the sheet is not less than three hundred and 
 fifty feet. 
 
 “On the low hills on either side of the road, at no very great distance from the 
 Leap Post Office, a bed of fine-grained, yellowish-white, ashy sandstone, with scarcely a 
 trace of bedding, is seen to overlie the sandstones and shales. (Plate 46, fig. 1.) From 
 
 
 
 * On the Age of the Mesozoic Rocks of the Lake Eyre Basin. Proc, Austr, Assoc, Adv. Set., i, 
 1888, p. 228. 
 + Brisbane: by Authority : 1889, 
 
 
 
 ——- -—, 
 
547 
 the similarity of the components of these sandstones to those of the Mandarana lavas, 
 and their apparent unconformability to the underlying rocks, they are regarded as being 
 subaqueous trachytic tufts of the same age. 
 
 “ Another fragment of rock of this class is seen capping the Finlayson Hills, 
 twenty-two miles north-west of Mackay, and about a mile and a-half from the sea- 
 coast, where it forms a sugarloaf-shaped peak, resting on granite, and rising to a height 
 of about one hundred feet above the summit of the hills. (Plate 46, fig. 2.) This rock 
 has a matrix of a purple-grey hue, with well-marked banded or ribboned structure, in 
 which the lines of flows can often be seen to bend round the larger sanidine crystals 
 embedded in the base. As a whole, the rock is much more compact than the Mandarana 
 trachyte, and, like it, forms rudely hexagonal columns. 
 
 “On the eastern bank of the Victor Creek, in Selection 590 (Parish of Ossa), a 
 well-marked escarpment of trachyte, forming McKenzie Crags, occurs. Here the lava 
 rests upon the volcanic series.* Several other isolated fragments occur near highwater 
 mark at Rocky Bluff, aboat four and a-half miles south of Cape Hillsborough. 
 Near the head of-Niddoe’s Creek, one of the watercourses draining the western side 
 of that range of hills lying between the main range and the coast, a trachyte lava of 
 a somewhat different character is seen, dipping south-east at an angle of 12°, and 
 resting upon the sedimentary rocks of which this range is made up. Lithologically, 
 the rock may be called a quartz-trachyte, and throughout it presents a great uniformity 
 in its physical characters; it is made up of a light-grey porous matrix, in which 
 
 quartz, sanidine, and small specks of what appear to be hornblende are embedded. 
 “Tn the Parish of St. Helens, on the south bank of Alligator Creek, a lofty range 
 of mountains, the ‘ Pinnacles,’ which form a ‘corry,’ encircling one of the branches of 
 this creek, a great thickness of lava occurs. The rocks are trachytes of a brownish-grey 
 colour, and with which fine-grained trachyte tuffs are associated. The lava sheets have 
 their steeper faces southwards, and appear to dip in a general northerly direction. 
 
 “One of the sources from which some of these lavas and ashes have been ejected 
 appears to be Mount Barren, a steep, triple-peaked mountain, the highest summit of 
 which is about 2,000 feet above sea-level, and which is almost surrounded by the head 
 waters of St. Helen’s Creek. The rock of which this mass is made up is greyish- white 
 in colour, and somewhat porous, with a mean specific gravity of 2°56. In the matrix 
 small crystals of sanidine and minute specks of a black mineral—probably hornblende 
 —can be recognised; throughout the whole of the mass the rock retains very much the 
 same character. The mountain rises perpendicularly from the alluvial flat on the north 
 bank of St. Helen’s Creek, and in Barren Creek the mass is seen to be intrusive 
 through an ‘ orthoclase porphyry,’ upon which the sedimentary strata [of the Bowen 
 River Series] are seen to rest. No perceptible amount of alteration was detected in 
 any of the sections in which its intrusive character was observed. 
 
 “ Another denuded wreck of an ola voleano is to be found in Mount Jukes, some 
 1,800 feet above sea-level, and situated on the bank of Neilson’s Creek, and abou 
 twenty miles distant from Mackay in a north-westerly direction. The mean specific 
 gravity of the rock, from specimens in different parts of the mountain, was found to be 
 2°55. Different parts of the mass present different characters, but generally two 
 varieties can be recognised :— 
 
 (a) A coarse-grained rock in which a matrix can scarcely be said to exist, and 
 
 (6) A second in which crystals of sanidine and plagioclase are embedded in a 
 micro-crystalline base, which, with the aid of a lens, is seen to be made up 
 of small crystals and crystalline grains of sanidine and hornblende (°). 
 
 
 
 * At the base of the Bowen River or Permo-Carboniferous Formation. 
 
548 
 
 The former variety, owing to its coarse grain, would be called a nevadite, whilst the 
 latter would be best described by the term sanidine trachyte: both, however, are 
 merely varieties of one and the same rock. The rock is intrusive through the volcanic 
 series, and sends out here and there dykes of no great thickness and of a somewhat 
 similar character to the rock forming the main mass; hardly any apparent alteration 
 has taken place in the rocks through which the mass has burst. 
 
 “On the north side of the Bowen Road, near its crossing of Murray Creek, a 
 low hill opposite to Mount Ossa, known as Hammel’s Hill, is found to consist at its 
 base of a coarse volcanic ash or agglomerate, made up of trachytic materials, and above 
 which a rock not unlike that forming the ‘Sugarloaf’ at Seaforth lies. This, seen in a 
 bare scaur visible from the road, shows fluxion structure to the unaided eye, and in 
 places fragments of the ash appear to have been caught up in the lava when in a molten 
 condition, and dragged along with the viscid mass. The whole rock subsequently has 
 been pierced by a fine-grained granite, and the agglomerate much altered, rendering it 
 often, except on its weathered face, a matter of some difficulty to distinguish it from 
 some forms of the lava beds. 
 
 “The Scrubby Hill, Mount Ossa, behind the house in Selection 1585 is, judging 
 from the screes on its face, made up of a rock almost identical in physical characters 
 with that forming McKenzie Crags. 
 
 “As a whole, these rocks bear a remarkable resemblance to those of Mount 
 Britten. Some of the rocks there are very fine volcanic ashes, whilst others are true 
 lavas. The ‘ Stalk,’ a conspicuous pinnacle of rock on the divide between the waters of 
 the Fitzroy and the Burdekin, ‘ possibly one of the vents from which the volcanic 
 material of the bluffs in the neighbourhood of Mount Britten was ejected,’ * is almost 
 identical with the trachytes of Mounts Barren and Jukes. 
 
 “The Mount Britten rocks have been conjectured by Mr. R. L. Jack to belong 
 to the Desert Sandstone series, ‘whose base is often made up of similar volcanic dust.” 
 The Mount Funnel conglomerate, merely an outlier of this series, rests upon the 
 altered grits and conglomerates of Carbonifero-Permian [Permo-Carboniferous] age, 
 
 and is distant not less than forty-five miles from any rock its equivalent in age, © 
 
 and forms an impressive evidence of the power of denudation. 
 
 “The sedimentary rocks at Seaforth overlie a mass of porphyrite regarded as 
 being newer than those of the ‘ Volcanic Series,’ and which is well seen in a little bay 
 at Cape Aberdeen, a mile to the south of Cape Hillsborough. Here the porphyrite is 
 well seen in the cliffs at low water. It weathers into rude spheroidal masses, and where 
 a freshly-broken surface is examined it is often found to be amygdaloidal, the 
 greater part of the cavities being filled with carbonate of lime, though in some leucite 
 can be detected. 
 
 “Overlying the porphyrite, a thickness of grits and fine conglomerate, and, in 
 some places, nearly pure white and calcareous sandstones, occur. At one place directly 
 overlying the porphyrite a bed of ‘mudstone’ is seen. Some little distance north this 
 covers a great bank of conglomerate, which in turn is succeeded by the main mass of 
 grits, &e. 
 
 “The Cape Table-land is made up of about four hundred and fifty feet of 
 sedimentary materials, dipping at an angle of about 10° to W.S.W. The base con- 
 sists of a thick mass of cavernous and ferruginous sandstones, succeeded by whitish 
 conglomerates and breccias with thin beds of banded siliceous matter. Whether these 
 
 
 
 
 
 * Report by R.L,J. on the Geological Features of the Mackay District, p. 7. Brisbane: by 
 Authority; 1887, 
 
 a ae 
 
549 
 
 bands are formed by slow precipitation from springs charged with siliceous matter, or 
 are beds of fine volcanic dust subsequently cemented, there is no evidence, at present, 
 forthcoming to show. Hot springs are frequently met with in those districts where 
 voleanic action is or has been rife ; hence the siliceous bands occurring among the beds 
 of the Cape may only be the indirect result of that activity which is conjectured to have 
 taken place in the earlier stages of this period.” 
 
 Mr. H. Y. L. Brown* thus describes the Cretaceous rocks as seen by him 
 between the 139th parallel and the Queensland Boundary from Lat. 26 to Lat. 82 8.:— 
 
 “ The strata consist of brittle clays and calcareous shales, with bands of limestone 
 and gypsum, clay, ironstone and ferruginous sandstone, and sandy beds; they are, as a 
 rule, originally horizontal or gently undulating, and have a thickness, so far as at present 
 known, of three hundred feet to four hundred feet. Overlying this formation are beds 
 of sandstone, argillaceous sandstone, kaolin, grit, and pebbly conglomerate, forming 
 table-lands and hills almost invariably capped by a thin bed of yellow and red flinty 
 quartzite or jasper-rock, the total thickness varying from one hundred to two hundred 
 feet. The pebbles found in this conglomerate consist of agate, jasper, chalcedony, opal, 
 and coloured quartz, flint, white and crystallised quartz, and fossil wood showing a 
 brilliant polish or glaze. The composition of these Supercretaceous beds is the same 
 over wide areas, from the Warrego, in New South Wales, to the Diamantina. The 
 topmost bed of yellow flinty quartzite or porcelainised sandstones, which forms the 
 capping of the table-land formation, varies in thickness from ten to thirty feet; it has a 
 conchoidal fracture, and sometimes shows an amorphous structure, at others encloses 
 grains of sand or quartz pebbles (often coated by hyalite and opaline quartz), in which 
 ease it may be considered a conglomerate. This porcelainised rock is intensely hard, 
 and its particles are at a tension; the most common appearance it presents is that of 
 hard red or yellow boulders fitting close together, splintered, cracked and jointed into 
 rounded and roughly prismatic shapes. It lies in patches on the argillaceous sandstones 
 and clays, forming in some places a mere coating, in others a deposit of thirty or forty 
 feet thick. Large and small cellular boulders and slag-like masses, with hollow 
 stalactitic forms, are often found. Whether in masses or pebbles the rock is invariably 
 glazed, so as to present a shining red or yellow surface. The most likely theory that 
 can be advanced to account for the formation and glazed surface of this rock is that it 
 has been formed by the infiltration of siliceous water from hot springs into beds of loose 
 sand or porous sandstone. The stalactite-like forms of some of the specimens from 
 Cooper’s Creek, the occurrence of siliceous cores round nuclei of cemented sand in 
 loose sand, and fragments of quartzite cemented together by silica, seem to prove this. 
 The downs which flank the table-lands and hills are undulating and level plains, covered, 
 as a rule, with a pavement-like coating of blocks or pebbles, or a red and yellow glazed 
 porcelainised quartzite and flinty rock resting on soft yellow and reddish clayey loam ; 
 the glazing of these stones is also probably due to the action of siliceous water. The 
 table-lands and hills composed of these Supercretaceous rocks are elevated to a height of 
 some one hundred to two hundred and fifty feet above the level of the surrounding 
 plains ; though generally horizontal they are sometimes inclined at a low angle. Onthe 
 Nilpie Nilpie Creek the flinty quartzite forms steep bluffs, and also occupies the creek- 
 flat below, and undulates beneath the soft silt flats. . . . The elevated table-lands 
 and hills occupy the country north and south of Cooper’s Creek, in the vicinity of the 
 eastern boundary line [of South Australia] to Haddon Station, near which place the 
 range branches off eastward and northward into Queensland; Kirby’s Knob, Mount 
 
 * Report of Government Geologist. Adelaide: by Authority ; 1888, 
 
550 
 
 Kingsmill, Edinboro’ Castle, and Kertietia Hill being some of the chief points of 
 elevation. The Grey Ranges of New South Wales and Queensland belong to the same 
 formation. 
 
 “ Overlying the Cretaceous and superincumbent hard rocks are deposits of 
 loose and consolidated clay, loam, silt, sand, gypsum, limestone, &c., all of Tertiary and 
 Recent age. 
 
 ‘“‘Strewed over the surface of many of the plains and flat areas lie fragments of 
 gravel, ferruginous sandstone and quartzite, with agates, chalcedony, and other pebbles 
 derived from the table-hill formation, which prove the existence of these beds beneath 
 the surface at no great depth.” 
 
 It will be seen that Mr. Brown does not distinctly aver that the “ Super-Cre- 
 taceous”’ rocks described by him lie unconformably on the Cretaceous ; there can be no 
 doubt, however, that he so understands their relations, as is evident from the sections 
 accompanying the report. The identity of the “ Super-Cretaceous ” of South Australia 
 with the Desert Sandstone of Queensland, in Mr. Brown’s mind is settled by his remark 
 that “the Grey Ranges of New South Wales and Queensland belong to the same 
 formation.” The “ porcelainised” condition of a portion of the sandstone on the South 
 Australian side of the border is a very interesting observation, in view of the “ quasi- 
 vitreous’ appearance of the formation at Cloncurry and Croydon on the Queensland 
 side. The superposition of Tertiary rocks on the Desert Sandstone of South Australia 
 is an observation of the highest importance, as direct evidence of this nature is quite 
 wanting in Queensland, and Daintree ascribed a Tertiary age to the Desert Sandstone 
 itself. 
 
 Mr. Brown, in a Report to the Under Secretary for Mines of New South Wales, 
 dated 17th Oct., 1881,* observes that in the Mount Poole district [in the N.W. corner 
 of New South Wales] the Cretaceous Formation “forms the undulating plains or downs 
 of what was formerly known as the ‘Stony Desert,’ and is capped by the table-hills of 
 the Grey and Mount Stewart Ranges, which rise in steep escarpments aboveit . . . 
 Resting on the soft Cretaceous Formation, in outlying hills and tablelands, and in some 
 cases covering it, over large areas, is a series of kaolin, sandstone, grit and pebble- 
 conglomerate beds, capped by a layer of quartzite boulder-conglomerate, having often a 
 slight dip in various directions, but being generally horizontal. The pebble-conglomerate 
 is formed of large rounded boulders and pebbles of a yellow or reddish colour, together 
 with yellow flint, quartz, &c., porcelainised in some way or other to an intense hardness, 
 and bearing the appearance of having been fused. The total thickness from the bottom 
 of the kaolin and sandstone to the top of the quartzite averages about one hundred feet. 
 Mount Poole itself is an outlying mass of quartzite and flint conglomerate, forming a 
 capping on ferruginous yellow and white sandstone resting on Cretaceous marly clay 
 with gypsum ; as also are The Turrets and other hills near. Near Whampa Waterhole, 
 close to the 215-mile post on the N. S. Wales and Queensland boundary line, there is a 
 section of about two hundred feet caused by the falling away of part of an isolated 
 hill, as follows :— 
 
 (1.) Hard flinty quartzite. 
 
 (2.) White kaolin and sandstone, with veins of gypsum. 
 (3.) Gray marly clay, with gypsum nodules. 
 
 (4.) Yellow marly clay, with thin bands of clay iron ore. 
 
 
 
 
 
 * Legislative Assembly Paper, N.S.W., 4th Nov., 1881. 
 + Nos. 3 and 4 probably in Cretaceous, and Nos. 1 and 2 in “‘ Super-Cretaceous,” according to Mr 
 Brown, or Desert Sandstone according to Daintree’s nomenclature, 
 
551 
 
 “The continuation of the range whereof this hillis an outlier, extends north- 
 wards into Queensland and southward to Mount Stewart, and to the eastward of 
 Milparinka. A portion of this range near Tipperberry Creek has a claystone-con- 
 
 glomerate instead of quartzite forming the capping of the hills, the lower beds being the 
 same, 
 
 ** At Mount Stewart the section is:— 
 
 Ft. in. 
 
 (1.) Quartzite conglomerate ... : 6 ee 10 O 
 (2.) Yellow sandstone, with grit and, pebble ‘conglomerate ‘a 20 O 
 (3.) White kaolin and sandstone _... out ae sa ; 
 
 (4) Pink, : le dace ae es 
 (5.) Gray marly clay, with iron ore and gypsum merging into the plains.* 
 
 “The Grey Range enters Queensland about eight or ten miles to the west of 
 Whampa, and is of the same formation but of larger extent than the last mentioned. 
 
 “On the top of one of these small tablelands, eight or ten miles south-west of 
 Whampa, there isa grove of fossil tree-stumps standing in an upright position. There 
 are thirteen or fourteen large ones, the greatest diameter being about four feet, 
 and the height four and a-half feet. The woody portion is represented by a white 
 quartz rock, and the bark by a brown quartzose sandstone and grit. Many of them are 
 hollow, and fragments are lying about in all directions. Originally they must have 
 been covered up, while erect, by a deposit of mud or other soft material like that on 
 which they grew, and became petrified by the infiltration of silica and deposition of sand 
 in their hollow portions; the matrix having since been denuded, they stand as evidences 
 of how trees have degenerated in size in this part of the country since Cretaceous 
 times. 
 
 “ These hills extend a long distance westward and south-west. The Sisters, 
 Mount Shannon, and many other flat-top hills, are of the same formation, which thins 
 out to the south towards Mount Arrowsmith and the other outcrops of Silurian and 
 Devonian rocks. 
 
 “Near Mullyeo and Killara Run there is a section showing quartzite con- 
 glomerate on pebble conglomerate, with a deposit of chalky limestone conglomerate at 
 the base of the hill, pieces of which, together with flint and chert, are contained in it. 
 Quartzite conglomerate hills of low elevation extend from Mullyeo to the Warrego, and 
 up both sides of that river beyond Yantaballa on one side, and Shearers Springs on the 
 other, into Queensland. What may be the geological age of those beds is not known, 
 other than that they overlie deposits of Cretaceous age, as no fossils have been found 
 in them. It is possible that they are upper beds of the Cretaceous period. They 
 occupy the same position as the Queensland Desert Sandstone of Daintree, which has 
 been lately proved by Mr. Jack, Government Geologist of Queensland, to be of 
 Cretaceous age. 
 
 “‘ Nearly the whole surface of the Downs country in the neighbourhood of Mount 
 Poole, and particularly the soft Cretaceous plains, is covered with a layer of angular and 
 rounded stones, consisting of quartz, slate, sandstone, limestone, flint, ironstone, trap, 
 quartzite, jasper, chalcedony, gypsum, and fossil wood. Near the Silurian ranges these 
 fragments are generally quartz and slate, directly derived from the ranges, while on the 
 plains they are quartzite, sandstone, &c., derived from quartzite and sandstone con- 
 
 glomerate, which at one time covered this area, and of which the table hills and ranges 
 alone remain. 
 
 
 
 * The dividing line between the Cretaceous and “ Super-Cretaceous” rocks is probably the base of 
 No, 4 in the above section. 
 
552 
 
 In a “ Report on a Journey from Adelaide to the Hale River” * Mr. Brown 
 refers to the prevalence of “ Cretaceous clays and shales overlaid by sand and Super- 
 Cretaceous rocks in the form of tablehills and tablelands” from Finnis Springs to Anna 
 Creek, and from Anna Creek to Algebuckina on the Neales River. “ From Mount 
 Dutton northward to the vicinity of Mount Burrell, some two hundred and fifty miles, 
 the whole country is occupied by the Cretaceous and Tertiary formations.” 
 
 “The tableland, tablehill, sandhill, plain, and stony downs country presents a 
 very similar aspect all over the area occupied by it. . The jasper rock and porcelainite, 
 or Desert Quartzite, forms the uppermost bed or capping of all, or nearly all, the flat- 
 topped hills. This rock seems to have been formed by the infiltration of silica into the 
 sands or sandstone and clay beds, which have been converted into jasper and porcelainite. 
 The same will also occur in dykes in the sandstone and older rocks, and in many places 
 has the appearance of having been deposited from springs. Travertine limestone and 
 brown iron ore, which occurs as cappings to the flat-topped hills, and in large masses, 
 have apparently been deposited in this way, as they can be seen directly connected with 
 the present springs, although to a limited extent. 
 
 “Fragments of these rocks—viz., jasper, porcelainite, quartzite, and brown iron 
 ore, together with flint, common opal, and opaline quartz—are scattered over the 
 Cretaceous Clay plains and tablelands forming what are known as ‘Stony Downs.’ 
 The sandstone forming the lower parts of the tablehills also contains pebbles and 
 boulders of quartz, quartzite, and other waterworn siliceous pebbles, which are also in 
 many places thickly scattered over the Plains. The thickness of these Super-Cretaceous 
 (or Tertiary) rocks varies greatly. They become thicker in going north.” 
 
 It will be noticed that the Writer now refers to the ‘‘Super-Cretaceous’”’ as Tertiary- 
 
 Mr. Brown, in a “‘ Report on the Country between Port Augusta and Eucla,” ¢ 
 refers to “horizontal beds of Desert Quartzite, grit, conglomerate, sandstone, and kaolin, 
 identical with the beds constituting the table-hills of the Cretaceous Formation,” seen 
 capping the lower portions of the granitic and metamorphic Warburton Ranges. 
 
 Between Kingoonya and Coondambo (north of Lake Gairdener) red loams and 
 sandy plains alternate with stony downs and tablelands of desert quartzite. 
 
 Mr. Brown’s latest views on the Desert Sandstone, as developed in South 
 Australia, are given in a paper “On the Mesozoic Plains of South Australia, &c.,” read 
 in Section C, at the Sydney Meeting (1888) of the Australian Association for the 
 Advancement of Science.§ After describing the “ Lake Eyre Basin ” and other regions 
 consisting of the Rolling Downs Formation, Mr. Brown says :— 
 
 “The tableland and tablehill country occupy a large area in many places, as in 
 the north-east corner of the colony. The general elevation above the plains is about one 
 hundred to two hundred and fitty feet, the upper bed is almost invariably a yellow flinty 
 jasper rock, or porcelainized sandstone and quartzite, varying in thickness up to thirty 
 or forty feet. Sometimes it is a conglomerate, and at other times a sandstone. It rests 
 on sandstone, argillaceous sandstone, kaolin, and grit, with thin bands of a loose pebble 
 conglomerate. The pebbles found in the conglomerate consist of agate, jasper, 
 chalcedony, opal, coloured quartz, flint, white and crystallized quartz, and fossil wood, 
 all showing a brilliant polish or glaze. 
 
 ‘“‘ As these tablehills generally have sharp, well-defined cliffs and escarpments, the 
 stratification can be easily studied. They are either of Upper Cretaceous or Lower 
 Tertiary Age, and rest directly on the upper beds of the Cretaceous Formation, in 
 horizontal and sometimes gently inclined layers; their composition and arrangement is 
 
 
 
 * Adelaide: by Authority : 1889. + South Australian Legislative Assembly Paper, 9th July, 1885. 
 + Approx. Lat. 30° 50’ S. ; Long. 134° 40’ E. § Proc. Austr. Assoc. Adv. Sci., 1888, 1., p. 241. 
 
553 
 
 the same over wide areas in South Australia, New South Wales, and Queensland, as far 
 east as the Warrego River, where I have had an opportunity of examining them. The 
 topmost bed of jasper rock has generally a conchoidal fracture and amorphous structure, 
 although sometimes containing grains of sand and pebbles, and becoming a conglomerate ; 
 it also occurs as rounded fragments and pebbles of yellow jasper rock cemented together 
 in masses with glazed surfaces. 
 
 “The Stony Downs are undulating and level plains, flanking the tablelands and 
 extending for miles over the country, and covered with blocks and pebbles of the flinty 
 jasper and other siliceous rocks, with sometimes vein quartz, slate, and sandstone ; these 
 fragments of rock are scattered over the surface of the plains and rest on soft yellow and 
 reddish clay loam, derived from the denudation of the underlying shales. In many 
 places the ground is covered with a smooth pavement-like covering of glazed fragments 
 and pebbles, as in the Stony Desert of the Diamentina; in others the jasper rock lies 
 scattered in slag-like masses and lumps on the soft loamy surface of the plains, together 
 with gravel, shingle, and fragments of agate, chalcedony, quartz, flint, &c. It is difficult 
 to account for the even distribution of these gravel and rock fragments over such a large 
 extent of plain surfaces, floating ice being the only agent likely to produce such results. 
 Below and surrounding the tablehills and stony downs are the soft silt plains, which, 
 together with the former, cover the gypseous clays, maris, calcareous shales, limestone, 
 sand, and gravel drifts of the Cretaceous age.”’ 
 
 The late Rev. Julian E. Tenison Woods held that the Desert Sandstone was of 
 sub-erial or eolian origin, and was deposited in the position and at the levels at which 
 it is now met with. In a Paper “On the Hawkesbury Sandstone,’ read before the 
 Royal Society of New South Wales in 1882,* speaking of the views of Messrs. 
 Darwin, Daintree, Clarke, and Wilkinson, regarding the Hawkesbury Sandstone, but 
 applying his remarks also to the Desert Sandstone of Queensland, Mr. Woods observed :— 
 
 “One fact seems to be lost sight of in all these theories, and ‘that is that there 
 has been no upheaval. The beds are horizoutal in nearly every case, and there has been 
 very little alteration of level since they were deposited. This is true wherever the 
 formation is found, and it is a most significant fact connected with our eastern mountain 
 range. The highest portions are recent volcanic, granitic, or horizontal sandstones, 
 which have not been upheaved from the sea. There has been evident depression about 
 such places as Sydney Harbour, but no elevation anywhere.” 
 
 Again, in the same Paper, Mr. Woods observed :—“ I do not think that the 
 denudation [of the Desert Sandstone] has been very great, for most of these aérial hills 
 were never united. It used to be the custom to refer the small horizontal caps and 
 outliers on the tops of mountains to the remains of an enormous formation which had 
 been denuded away. I myself thought this of O’Connor’s Nob,+ near Cooktown, and 
 Mount Pigeonhouse, near Jervis Bay. Such stupendous denudation on horizontal 
 strata, without any upheaval or subsidence, baffles comprehension ; but when the aérial 
 origin of these outliers is understood, the difficulty vanishes. There has been little or 
 no denudation. The sandstone has been deposited just where it is found, and was 
 never much larger than we see it now.” 
 
 Had Mr. Woods lived to hear of Mr. Maitland’s discoveries of an abundant and 
 identical marine fauna foundat high levels in the different fragmentary tablelands of Desert 
 Sandstone, in the neighbourhood of Cooktown, I have no doubt that he would, with his 
 well-known candour, have admitted the cogency of the evidence in favour of elevation. 
 
 
 
 * Journ. R. Soc. N.S. Wales, 1882, xvi., p. 53. 
 
 + **Connor’s Nob.” (R.Z./.) 
 
 +I can testify that, during the severe illness from which he never recovered, Mr. Woods in a very great 
 measure abandoned the olian theory of the origin of the Hawkesbury and Desert Sandstones, (2.2£. Jun.) 
 
554 
 
 It may be noticed, from the first paragraph above quoted, that Mr. Woods appeats to 
 have confounded elevation with disturbance, or at least to have considered the one as 
 necessarily accompanying the other. I fear that it will continue “to be the custom” to 
 attribute such phenomena as Mr. Woods referred to, to elevation and subsequent 
 denudation. So far from “such stupendous fecqeae a on horizontal strata” baffling 
 comprehension, the earth is so full of examples of the same kind, that they may be said 
 to be part of the everyday experience of every geologist. It is only necessary to 
 instance the Cafions of Colorado, the Felsenstadt in the Riesengebirge and the Blue 
 Mountains of New South Wales, and I venture to say that most of my readers can 
 supply other instances from their own observation. 
 
 The Upper Group of the Cretaceous Rocks, or Desert Sandstone, was, until recently, 
 regarded as almost unfossiliferous. Organic remains appear to have been first found in 
 these strata in 1872, by Mr. Norman Taylor, at Battle Camp, near Cooktown. In 1885, 
 Mr. Warden Samwell collected fossils from the Desert’ Sandstone at Croydon, and 
 subsequently the Writer made further collections from the same district. In 1890, 
 Mr. A. Gibb Maitland discovered fossils in the Desert Sandstone near Battle Camp 
 Range, on the Cooktown and Palmer Railway. But even of more importance than these 
 is the history of the Maryborough Beds, which, formerly regarded only as a portion of 
 the great Cretaceous Series, are now known to occupy a higher position, representing 
 the Desert Sandstone of other parts of Queensland. The organic remains of the Desert 
 Sandstone and Maryborough Beds, my Colleague says, ‘‘ partake in a great measure of 
 the facies.of the Rolling Downs Formation, with an admixture of forms not hitherto 
 recognised in the latter.” 
 
 AGE OF THE DESERT SANDSTONE AND LIFE OF THE PERIOD. 
 
 The following is my Colleague’s List of Fossils from this Formation. The 
 different localities are denoted by initial letters, as follows :— | 
 True Blue Hill, Croydon, 7; Bett’s Creek (Cape River), B; Mitchell River, mr; Mount 
 
 Angus, Croydon, A; Maryborough, M; Mullet Creek, mc; Isis River, 1; the first four localities being in 
 the Desert Sandstone proper, and the last three in the Maryborough Beds, 
 
 
 
 PLANTA. | Maceoyella? umbonalis, Moore a M 
 Acory.EDoNEs. | Cucullea robusta, Eth. ... sa a M 
 Didymosorus? gleichenioides, Oldham Nucula quacraga, Bul, = 
 ead Marne iF = | » gigantea, Eth. ... M, MC 
 Glossopteris, sps. a “e BME | Nuculana (? Yoldia) Randsi, Eth. fil. I 
 | <Adrana elongata, Eth. ... M 
 ANIMALIA. | Lrigonia nasuta, Eth. ee M 
 ECHINOIDEA. | » sp. ind. (a.) (Pl. 26, fig. 5) M 
 Micraster Sweeti, Eth. fil. 0... mu Cyprina Clarkei, Moore .. vee M 
 Unicardium ? Ltheridgei, Eth. fil. va M 
 Bracutoropa. Paicomera marieburiensis, Eth. Be M 
 Rhynchonella croydonensis, Eth. fil. ... TA } ? sp. ind. (Pl. 26, fg. a M 
 PELECYPODA. | Glycimeris sulcata, Eth.. M 
 . Moore M 
 Ostrea, sp. ind. (Pl. 48, fig. 8) ... om T fe he ea 
 2 
 
 Placuna, sp. ind. (Pl. 43, fig. 9) oe ra ae. *P- ro (EL 26, Be. 2) x 
 Lima (Radula) Radsi, Eth. fil. {a ALEMGE a we *P. s Pl. 43, t 1 1 hos 
 reine Hie) © a taal eredo, sp. ind. ( gs. 11 and 12) at 
 
 Pseudavicula, alata, Eth. ti ; uM | GASTEROPODA. 
 Macceyella pone var. mariceburiensis, Siphonaria Samwelli, Eth. fil. ... ais a. 
 He fil. Peay nee ee Natica variabilis, Moore 4 os M 
 
 corbvensis, Moore... tee M 
 
 mn reflecta, Moore ots ee IT «| CEPHALOPODA. 
 
 a ? substriata, Moore Nie mM | Belemnites, sp. wie te ate M 
 
 
 
555 
 
 To the foregoing list there are to be added the fossils from the Cooktown and 
 Palmer Railway, collected by Mr. Maitland, as already mentioned. Mr. Maitland refers * 
 to Maccoyella ? and Rhynchonella, but the collection has not yet been examined by my 
 Colleague, and so far as we know, adds no new species to the Desert Sandstone list. 
 
 Of the above, the following species of Pelecypoda are common to the Desert 
 Sandstone (including the Maryborough Beds) and Rolling Downs Formations; 
 Maccoyella Barklyi, M. reflecta, M. umbonalis, M. corbiensis, M. substriata, Nucula 
 quadrata, Cyprina Clarkei, and Glycimeris rugosa, and also the Gasteropod Natica 
 variabilis, and the following genera—Rhynchonella, Ostrea, Lima, Pseudavicula, 
 Maccoyella, Cucullea, Nucula, Trigonia, Cyprina, Paleomera, Glycimeris, Pecten, 
 Natica, and Belemenites ; so that a strong case can be made out in favour of a connection 
 between the Rolling Downs and Desert Sandstone. It must, however, be remembered 
 that the original fossils from Wallumbilla, Mount Abundance, and Mount Corby, upon 
 which several of the above identifications rest, were collected without any idea that a 
 distinction could be made between the Desert Sandstone tablelands and the underlying 
 Rolling Downs Formation. It is just possible, therefore, that some of the fossils quoted 
 as belonging to the Rolling Downs ought to be credited to the Desert Sandstone. 
 
 In the above list we have an assemblage of fossils of decidedly Cretaceous types, 
 and possessing much in common with the Rolling Downs Formation. We may therefore 
 with safety separate the Cretaceous rocks met with in Queensland into a Lower and 
 Upper Series, the latter being our Desert Sandstone, which is separated from the Rolling 
 Downs Formation by an unmistakable unconformability. At the time when Mr. 
 Daintree and Mr. R. Etheridge, F.R.S., wrote their Papers on the Geology and 
 Paleontology of Queensland (1872), no determinable fossils had as yet been obtained 
 from the Desert Sandstone, but the Maryborough Beds had yielded a considerable 
 number, on the strength of which Mr. Etheridge placed the latter beneath the 
 Hughenden and Marathon beds. We now unite the Desert Sandstone and Mary- 
 borough Beds, on the ground of the similarity of their organic remains, and the Desert 
 Sandstone has been observed to rest unconformably on the Hughenden Beds. Taking 
 this break into consideration, Daintree regarded the Desert Sandstone as Tertiary. The 
 fossils which, in the last few years, have been discovered in the Desert Sandstone at 
 Croydon and Cooktown show that the formation has much in common with the Rolling 
 Downs or Lower Cretaceous, and nothing in common with the Tertiary. Lithologically 
 it has always seemed to me that the well-consolidated and occasionally quasi-vitrified or 
 porcellanised strata of the Desert Sandstone were singularly unlike any of the compara- 
 tively loose and unconsolidated deposits ascribed in Australia to the Tertiary age. The 
 late Rev. J. E. Tenison Woods even went so far at one time as to regard the Desert 
 Sandstone, on the ground of lithological similarity, as the equivalent of the Hawkesbury 
 Sandstone—which, however, is quite untenable in the face of the fact that it is newer 
 than the Lower Cretaceous. Lithological resemblance in such a case does not count for 
 much, as one siliceous sandstone is very hke another, whatever may have been the date 
 of its deposition. 
 
 MINES CONNECTED WITH THE DESERT SANDSTONE. 
 
 The presence of coal in the Desert Sandstone is now well known. In a previous 
 portion of this chapter descriptions of the coal at Cooktown and in the Cape York 
 Peninsula have been given. 
 
 Speculations as to the existence of deep auriferous leads beneath the Desert 
 Sandstone will be found on page 539. 
 
 
 
 
 
 * And in all probability correctly 50. (RE. J unr.) 
 
556 
 
 Opals and other precious stones form at present the chief mineral wealth of the 
 formation. 
 
 The opals are found in nodules of ferruginous siliceous sandstone and siliceous 
 ironstone, either in the “Desert Sandstone” or denuded out of it, and lying on the 
 surface of the underlying “ Rolling Downs” formation. 
 
 T’rom the following places valuable opals have been obtained :— 
 
 ° / °o , 
 Pleasant Creek... vat .. S. Lat. 25 23 uae E. Long. 145 15 
 Bulgroo and Kyabra Creek site » 25 50 ond "7 143 35 
 Costello’s Creek .., axe a » 20 57 A 3 142 47 
 Mayne River ef ae oe ay By BY ee ii 141 32 
 Nickavilla ... on bg » 26 20 on +, 144 20 
 Winton ... nie saa aed peauod £P. Fr 143 12 
 Boulia » 22 55 ee ; 143 0 
 
CHAPTER XXXIV. 
 
 THE ORGANIC REMAINS OF THE DESERT SANDSTONE FORMATION 
 (UPPER CRETACEOUS), 
 Wirn DESCRIPTIONS OF THE SPECIES. 
 
 Kingdom—PLANT. 
 Section—CRYPTOGAMIZ. 
 CLASS—ACOTYLEDONES. 
 
 Order—FILICES. 
 Family—GLEICHENTACE. 
 
 Genus—DIDYMOSORUS, Debay and Ettingshausen, 1859. 
 (Denk. K. K, Akad. Wissensch. Wien, xvii., 1 Abth., p. 186.) 
 
 DIDYMOSORUS ? GLEICEENIOIDES, Oldham and Morris, var. 
 
 Pecopteris (Gleichenttes) linearis, O. and M., Mem. Geol. Survey India, ii., p. 324. 
 gleichenioides, O. and M., Pal. Indica (Gondwana Flora), 1862, i., Pt. 1, p. 45, t. 25, 
 Un atntig lheas 
 Gleichenites (Gleichenia) bindrabunensis, Feistmantel, Ibid., p. 93. 
 Gleichenia bindrabunensis, Schimper, Traité Pal. Vég., 1869, ii., p. 670. 
 Didymosorus ? gleichenioides, Etheridge fil., Proc. Linn. Soc. N. 8. Wales, 1888, iii., Pt. 3, p. 1808, 
 t. 38, f. 3. 
 
 Sp. Char. Frond [bipinnate] long, narrow, parallel-sided, tapering but very 
 slowly. Pinnze long and linear, opposite or sub-alternate, rarely alternate, obtusely 
 pointed at their apices, springing from the rachis at right angles, and in close contiguity 
 to one another. Rachis straight, non-flexuous, small and delicate. Pinnules short, 
 entire, broad-ovate, sub-alternate on the pine, and decurrent. 
 
 Obs. The present plant is, I believe, identical with the Pecopteris gleicheniovdes, 
 Oldham and Morris, which should be placed in the genus Didymosorus, Debey and 
 
 ? ‘ I : 5 y Ng 
 Ettingshausen,* one of the Gleicheniacee. This genus resembles the recent Gleichenia 
 but possesses a different fructification. The frond in Didymosorus is dichotomous and 
 bipinnate, each division being very long, narrow, and nearly parallel-sided; the pinne 
 are quite linear, either opposite, or sub-alternate, on a very narrow rachis. 
 
 The typical species of Didymosorus, D. comptonifolia, D. and E., occurs in the 
 Cretaceous rocks of Aix-la-Chapelle, whilst Pecopteris gleichenioides is found in the 
 Mesozoic rocks of the Rajmahal Series of India. 
 
 The Australian plant corresponds with the description of the genus in every 
 particular, but we do not possess enough of the frond to show dichotomisation. It is 
 either identical with the Indian species, or a mere variety of it, although it has points in 
 common with the European form. Unfortunately for the purposes of strict identifica- 
 tion, the specimens are preserved ina fine siliceous grit, which has obliterated all evidence 
 of fructification, if any such existed, and also of the nervation. As regards size the 
 
 > ” 
 
 
 
 * Denks, K, Akad. Wissensch. Wien, 1859, xvii., 1 Abth., p. 186. 
 
558 
 
 specimens now under description agree entirely with the Indian species, but seem to be 
 rather smaller than the European, the general width of a pinna being two-sixteenths of 
 an inch. 
 
 The figures of Oldham and Morris* represent portions of fronds as long as seven 
 inches, and two and a-half inches wide, but the largest of our specimens is four inches 
 long and one and a-quarter wide. The pinne are certainly narrower than D. gleichenioides, 
 but as this point may entirely depend on the position occupied by the specimen in the 
 frond, it cannot be taken as a point of much importance. 
 
 As no fructification has been seen, it would perhaps be more advisable to place 
 the Croydon fossils, ‘characterised by the slenderness of the whole Jeaf, and by the 
 delicate linear form of the pinne”’ (Feistmantel), in Gleichenites, as Oldham and 
 Morris have done with their species; although, be it noted, they refer to the general 
 resemblance of the latter to Didymosorus. On the other hand, so close a resemblance 
 can hardly have existed without some corresponding affinity in the productive state, and 
 I shall therefore venture to place Gleichenites gleichenioides in Didymosorus, and pro- 
 visionally refer the Australian form to it. 
 
 The general relations of this peculiar fern have been ably discussed by the late 
 Messrs. Oldham and Morris; but in their description they state the pinne are alternate. 
 Their figures, however, show as much variation from alternate to opposite as do our 
 specimens. At the same time the pinne are apparently closer in the Indian fossils. 
 
 The small ovately-pointed pinnules, entirely deeurrent as they are, give to the 
 pinne a fret-saw-like appearance, and are evidently a very characteristic feature of the 
 fern. In consequence of the gritty nature of the matrix the venation is obscure, but 
 Oldham and Morris say generally—“ The nervation of the pinnules is very indistinct, 
 but seems to consist of a small flexuous midrib becoming nearly obsolete at the end of 
 the pinnules, and from which secondary veins pass off obliquely at irregular intervals.’ + 
 
 Loc. and Horizon. True Blue Hill, Croydon Gold Field, North Queensland 
 (R. L. Jack). 
 
 Family—DICTYOTANIOPTERIDZ. 
 
 Genus—GLOSSOPTERIS, Brongniart, 1828. 
 (Prodrome Hist. Veg. Foss., p. 54.) 
 
 Obs. The discovery of this genus by Mr. W. H. Rands, in beds believed to be of 
 the age of the Desert Sandstone, has already been referred to.t That the plant-remains 
 so discovered are portions of the fronds of Glossoptevis is unquestionable. The majority 
 I am simply unable to distinguish from G. Browniana, Brong., two at least possessing 
 the broad striated midrib represented in some of Dr. O. Feistmantel’s figures.§ With 
 these are portions of two other very large fronds, with fine close veins, which stream 
 out at a very low angle from the midrib, producing a long, narrow mesh, and recall to 
 mind the appearance of G. teniopteroides, Feist.,|| and G. ampla, Dana.{ - The large 
 size that these leaves unquestionably attained indicate the latter species as that to 
 which they are more nearly allied It will be remembered that both G. Browntana and 
 G. ampla occur in the Bowen River Series of the Permo-Carboniferous.** 
 
 
 
 
 
 * Pal. Indica (Gondwana Flora), 1860, i., Pt. 1, fas. 6, p. 45, t. 25, t. 26, f. 2 and 8. 
 t+ Loc. cit., p. 46. 
 
 + See pp. 169 and 193. 
 
 § Mem. Geol. Survey N. 8S. Wales, Pal. No. 3, 1890, t. 17, f. 1, la. 
 
 \| Ibid., t. 18, f. 1, 1a. 
 
 WI foid., t. 19, £. 1 and-2: 
 
 ** See pp. 193 and 195, 
 
559 
 
 This is the first occasion on which Glossopteris has been found in Australia 
 outside beds of Permo-Carboniferous age, z.e., beds which could be shown so to be by the 
 associated fossils. Hitherto, the occurrence of Glossopteris in our Paleozoic, and 
 Teniopteris in the Mesozoic strata, has been regarded as an article of faith, the first 
 never having been, to my knowledge, found above the Upper Coal Measures, and the 
 second plant below the Clarence Series. So long has this stood the test of inquiry in 
 the field, and so closely do the leaves found by Mr. Rands correspond to two of our 
 most characteristic Permo-Carboniferous species of Glossopteris, that were it not for a 
 personal knowledge of the extreme care and wide stratigraphical experience of my 
 Colleague and his Assistant, I should be tempted to question the reference of the beds 
 yielding these leaves to the Desert Sandstone Series. It must, at any rate, be regarded 
 as a very remarkable survival. In India, it is true, Glossopteris passes, according to 
 the stratigraphy of the late Dr. O. Feistmantel, into the Trias,* and the same appears 
 to be the case in South Africa. There the upward course of Glossopteris, with any 
 certainty, appears to cease, uccording to our previous knowledge of its range in time ; 
 for although a species has been described by Prof. Trautschold from the Russian 
 Cretaceous, and by Messrs. Visiani and Massalongo from the Italian Tertiary,} still, 
 these determinations require confirmation. Perhaps the present instance may to some 
 extent supply this. 
 
 ' Mr. Norman Taylor, when acting as Geologist to W. Hann’s “ Expedition in 
 Northern Queensland,” as long ago as 1872, found Glossopteris in a tableland between 
 the Mitchell and Walsh Rivers, to which he in consequence ascribed, and with our then 
 knowledge justly so, a Carboniferous age, and it became known as “ Taylor’s Car- 
 boniferous Range.’’+ The tableland in question, however, according to my Colleague, 
 is a denuded fragment of the Desert Sandstone, and Mr. Taylor’s fossils must in conse- 
 quence be added to the list of the Desert Sandstone Flora. 
 
 Loc. Tableland south of Mitchell River (N. Taylor) ; Bett’s Creek, near Cape 
 Gold Field (W. H. Rands—Colln, Geol. Survey, Queensland). 
 
 Kingdom—ANIMALIA, 
 Sub-Kingdom—HCHINODERMATA. 
 Class—ECHINOIDEA. 
 
 Order— EU ECHINOIDEA, 
 Section—REGULARES (Endocyclica). 
 Family—SPATANGIDA. 
 
 Genus—MICRASTER, Agassiz, 1834. 
 (Prod. Mon. Rad. Echinod.) 
 
 
 
 MicrastER SWEETI, sp. nov. 
 
 Obs. It affords me much pleasure to associate with this, the first Mesozoic 
 Echinoderm described from Australian rocks, the name of my friend Mr. George Sweet, 
 of Brunswick, Melbourne, who has worked with much success amongst the fossiliferous 
 rocks of Eastern Australia, and to whom I am indebted for the contribution of a large 
 number of specimens. 
 
 
 
 * Mem. Geol. Survey N. S. Wales, Pal. No. 3, 1890, p. 119. 
 + Feistmantel, loc. cit., pp. 119, 120. 
 + Proc. R. Geogr. Soc., 1874, xviil., p. 92. 
 
560 
 
 Two previous but indefinite records of Cretaceous Echini have been made. In 
 1860, Dr. A. R. C. Selwyn wrote*: “I have lately discovered, embedded in our 
 Pliocene water-worn gravel, near Melbourne, fwo specimens, considered by McCoy to 
 belong to decidedly Chalk species. One is a very perfect Echinoderm, the other a 
 fragment of a Coral.” Such specimens have never been described by Prof. McCoy, but 
 he has referred to them in very emphatic terms in his Paper “On the Discovery of 
 Cretaceous Fossils in Australia,” wherein he remarks t: “ Mr. Selwyn also alluded 
 formerly to a specimen of an Echinide in flint given to him as found in sinking a well 
 at Prahran, near Melbourne, having been identified by Prof. McCoy as the European 
 Cretaceous Conulus albogalerus. The Author had also a flint Ananchytes ovatus of the 
 same age, given to him as found at Richmond, near Melbourne, also ; but he considered 
 both these specimens were unsatisfactory as far as the proof of their having really 
 belonged to any Australian stratum.” Nor is any reference made to these species in 
 Prof. McCoy’s second Essay “On the Recent Zoology and Paleontology of Victoria,” 
 under the section, ‘“‘ Cretaceous Period.” 
 
 The second reference is to a remark of the late Mr. Charles Moore, who, 
 speaking of a collection of West Australian fossils on view at an Exhibition, says §: “In 
 addition . . . . there was a silicious cast of a Micraster from the Chalk.” So far 
 as I am aware, no further steps have been taken to test the occurrence of this genus in 
 West Australia. 
 
 Few absolute particulars can be obtained from the present specimen, I regret to 
 say, from its bad state of preservation, beyond the fact that it is one of the Spatangide, 
 and probably referable to Micraster, but as neither the fascioles nor tubercles are visible, 
 the reference to this genus is even questionable. 
 
 The test, in its present state, is two inches long from anterior to posterior, and 
 one and a-half inches wide. It is spatangoid in outline, with petaloid ambulacra, the 
 anterior pair much the longest, odd or anterior ambulacrum reposing in the sulcus, 
 which evidently indented the anterior border. The specimen is a cast, the test having 
 been entirely removed. The whole of the abactinial surface is concealed in immovable 
 matrix. It will be subsequently figured. 
 
 Loe. Corporation Quarry, Maryborough (G@. Sweet—Colln. Sweet, Melbourne). 
 
 Sub-King¢dom—MOLLUSCA. 
 Section—MOLLUSCOIDA. 
 Class—BRaACHIOPODA. 
 Order—TRETENTERATA, 
 Family—RHY NCHONELLIDA. 
 Genus—RHYNCHONELLA, Fischer, 1809. 
 
 (Notice Foss. Gouv. Moscou, p. 35.) 
 RHYNCHONELLA CROYDONENSIS, sp. nov., Pl. 41, figs. 18 and 14. 
 Sp. Char. Shell moderately transversely elongated, wider than high, feebly 
 convex, and sometimes attaining rather large proportions ; cardinal margin angular; 
 front faintly sinuated. Ventral valve with a wide shallow sinus, and the flanks to some 
 
 
 
 * Quart. Journ. Geol. Soc., 1860, xvi., p. 148. 
 + Trans. R. Soe. Vict., 1866, vii., p. 50. 
 
 $ Ann. and Mag. Nat. Hist., 1867, xx., p. 195. 
 § Quart. Journ. Geol. Soc., 1870, xxvi., p. 227. 
 
561 
 
 degree flattened; umbo sharp and projecting; dental plates, as indicated by the 
 impressions left, strong, short, and rather eurved ; flanks bearing six prominent angular 
 ribs, and the suleus occupied by four fainter coste, with indistinct traces of distant 
 transverse lamelle. Dorsal valve depressed, with a faint flat fold; septum very short ; 
 coste similar to those of the ventral valve. 
 
 Obs. This Rhynchonella is common in the Croydon Grit, but always in the form 
 of casts, and those usually of the ventral valve. At first sight it would appear to have 
 some resemblance to R. lacwnosa, Schl., from the White Jura of Germany, although the 
 outline is decidedly more that of I. compressa, Sby., of the European Cretaceous, but 
 the coste in our shell are too few and coarse for that species. With the exception of 
 the inequilateral feature in Rhynchonella asteriana, D’Orb., our shell comes very close 
 to this. The specimens are not large for a Jurassic Rynchonella, but they are so as 
 compared with the generality of the Cretaceous forms, and when compared with 
 Tertiary or Recent species are very large. 
 
 Another shell allied to R. croydonensis is R. major, J. de C. Sby., sp.,* from tho 
 Upper Mesozoic Beds of Cutch, but the cost are far too numerous and close. 
 
 Associated with 2. eroydonensis is a smaller cast, apparently that of a dorsal 
 valve. It possesses a much more regular degree of convexity, and is without a mesial 
 fold, but there is present the same flattened umbonal region as in the above. Its more 
 convex form generally and the want of a fold forbids it being the dorsal valve of 2. 
 eroydonensis, but at the same time the two forms do bear an indescribable resemblance 
 to one another. As in the former case, the septum is short (Pl. 42, fig. 8). 
 
 Loe. True Blue Hill, Croydon Gold Field (2. LZ. Jack); Mount Angus, Croydon 
 
 (R. L. Jack). | 
 Section—MOLLUSCA VERA. 
 
 Class—PELECYPODA. 
 Order—OSTRACEA, 
 Family—OSTREID ZA. 
 
 Genus—OSTREA, Linneus, 1758. 
 (Syst. Nat., Ed. x., p. 696.) 
 OstrEa, sp. ind., Pl. 43, fig. 8. 
 
 Obs. Some obscure impressions and casts from the Croydon Grit appear 
 referable to this protean and widely spread genus. It is difficult to assign any definite 
 characters to them, but the casts are irregularly sub-obovate, oblique to some extent, not 
 greatly widening towards the front. The umbo of the under valve is thickened although 
 not curved upwards, but the left-hand edge or margin of the shell deeply sinuated. The 
 grooved cartilage area is roughly triangular, and obliquely inclined towards the sinuated 
 side. 
 
 This resembles many forms of Oyster, but is not unlike a variety of Ostrea 
 patina, which the late Mr. Meek proposed to call Ostrea subsinuata,t except that the 
 sinuated margin is on the right side of the attached valve; in our specimens it seems to 
 be on the left. In addition to this the ligamental depression is oblique, but in Meek’s 
 figure it is not so represented. 
 
 There is not sufficient evidence to warrant a specific name being given to these 
 specimens. 
 
 Loc. True Blue Hill, Croydon Gold Field (W. Samvel?). 
 
 * Trans. Geol. Soc., 2nd Ser., v., Expl. t. 22, t. 22, f. 16, 
 + Report U. 8. Geol, Survey Ter., 1876, ix. (Invert. Cret. Tert, Foss. Up. Missouri), p. 18, t. 11, 
 f. 4a and 4b. 
 
 2M 
 
 
 
562 
 Family —ANOMIID®. 
 
 Genus—PLAOUNA, Bruquiére, 1789. 
 (Encycl. Méthod., i.) 
 
 Pracuna, sp. ind., Pl. 43, fig. 9. 
 
 Obs. The presence of the genus Placuna in the uppermost Mesozoic Beds of 
 Queensland is shown by the occurrence of a small shell, one and a-quarter inch wide by 
 the same in height, with a nearly straight cardinal margin. The specimen is only an 
 impression, possibly of the interior of the right valve, and shows the indentations left by 
 its own diverging teeth, and the impressions of the teeth of the opposite valve. There 
 are also traces of the shoehorn-shaped muscular impression, but there is no sign of any 
 pit between the “ cartilage fulera.” 
 
 The transverse outline of this species renders it a peculiar one, as it is more or 
 less equal to the vertical measurement. 
 
 Loc. True Blue Hill, Croydon Gold Field (R. L. Jack). 
 
 Family—LIMID&. 
 
 Genus—LIMA, Bruguiére, 1789. 
 (Tab. Encycl. Méthod., Pl. 206.) 
 
 Tima (Rapvura) Ranpst, sp. nov., Pl. 21, fig. 18. 
 
 Sp. Char. Shell obliquely ovate, more or less compressed, very slightly alate 
 posteriorly. Huinge-line very short, straight, and horizontal. Anterior side rounded, 
 alate above, margin convex; posterior side small, very slightly alate, with a convex 
 margin, slightly emarginate above; posterior slope sharp; ventral margin obliquely 
 rounded. Umbones moderately acute, apparently incurved. Surface bearing as many 
 as fifteen (twelve to fifteen) broad, to some extent flattened, radiating ribs, with at 
 times traces of a few shorter interpolated costs, separated by flat interspaces, con- 
 siderably wider than the width of the ribs, crossed by delicate concentric lamelle; the 
 anterior and posterior wings, and the sides of the valves contiguous to them, are devoid 
 of ribs. 
 
 Obs. This shell, although allied to Lima Gordoni (P1. 24, fig. 16), is believed to 
 be distinct. The cost of the former are much more numerous, the margins of the 
 shell are quite differently curved, and there does not appear to be any pronounced 
 hinge-line. LZ. Gordoni is also much more obliquely produced towards the posterior 
 side. A fragment of another specimen would seem to show that some of the ribs on 
 the anterior side were spinous at their front edges. 
 
 From the shell I have called Oxytoma rochwoodensis (P1. 24, fig. 15) the present 
 differs in a less convexity, altogether different posterior wing and umbo, and by 
 possessing radiating ribs thicker and more obtuse. Our species resembles a shell 
 figured by Conrad as Lima leonensis,* but is less oblique. 
 
 Named in honour of Mr. W. H. Rands, Assistant Government Geologist of 
 Queensland. 
 
 Loc. Near Mullet Creek, twelve miles south of Rosedale Station, Port Curtis 
 (W. H. Rands); Corporation Quarry, Maryborough (W. H. Rands; G. Sweet— 
 Colln. Sweet, Melbourne; and 7. W. #. David—Colln. David, Sydney). 
 
 
 
 * Descrip, Cret, and Tert, Foss. Report U.S. and Mexican Boundary Survey, 1857, i., Pt. 2, p. 151, 
 t. 5, f, 3a-c, 
 
563 
 
 LIMA, sp. 
 NF e anita BE 
 
 Obs. A shell allied to this genus is perhaps represented in the ill-preserved 
 example represented in Pl. 21, fig. 11. The hinge has disappeared, but a small portion 
 of one of the ears remains. The exterior, as seen through the thin shell, is highly 
 cancellate, resembling that of Pecten equilineatus, Moore (Pl. 21, fig. 10). 
 
 Loc. Isis River, near Bundaberg, and Maryborough Road (W. H. Rands). 
 
 Order—MYTILACEA. 
 Family—A VICULIDZ. 
 
 Genus—PSEUDAVICULA, Etheridge fil. 
 (See p. 449.) 
 Obs. A description of this new genus comes more conveniently under the head of 
 “ Rolling Downs Fossils,” to which the reader is referred. 
 
 PsEUDAVICULA ? ALATA, Etheridge, sp., Pl. 24, fig. 14. 
 Avicula alata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviil., p. 342, t. 20, f. 8. 
 
 Sp. Char. Shell inequivalve, inequilateral ; auricles unequal, posterior much 
 expanded, anterior small; hinge-line straight, umbones acute and prominent, umbonal 
 region thick; valves with numerous (thirty-four) radiating ribs; with alternating smaller 
 ones, except near the middle of the valve, where the ribs (seven and eight) are all equal, 
 and range from the umbo to the ventral margin. (Ztheridge.) 
 
 Obs. The generic affinities of this species are at present very obscure. It is not 
 an Avicula, but may have relations with the present genus. 
 Loe. Maryborough (The late R. Daintree). 
 
 Genus—MACCOYELLA, Etheridge fil. 
 (See p. 451.) 
 Maccoyvetta BaRKLYI, var, MARIMBURIENSIS, Ltheridge fil. 
 Pl. 22, fig. 3; Pl. 42, figs. 4 and 5. 
 (For synonymy and description, sce p. 455.) 
 
 Obs. The species will be found fully described amongst the Rolling Downs 
 fossils ;* particular attention, however, may be called to Pl. 22, fig. 3, which seems to 
 be distinguished by the size and rugosity of the primary costw, and development of the 
 posterior spines. It is particularly characteristic of the Desert Sandstone Beds. 
 Other figures are given, Pl. 42. figs. 4 and 5, of specimens from Croydon. 
 
 Loc. Spring and True Blue Hills, Croydon Gold Field (R. L. Jack and W. 
 Samwell). Occurs also in the Rolling Downs Beds. 
 
 Maccoyretna corBiEnsis, Moore, sp. 
 Pl. 22, figs. 8 and 9. 
 Avicula corbiensis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 246, t. 11, f. 7. 
 Crenatula ? gibbosa, Etheridge, Ibid., 1872, xxviii., p. 339, t. 19, f. 3. 
 
 Obs. M. corbiensis nas been fully described under the “Rolling Downs” 
 section from specimens in the combined Collections of the Geological Survey and 
 Messrs. Tate, Sweet, and David. It is a particularly characteristic fossil of the 
 Maryborough Beds. 
 
 
 
 * See p, 455, Pl. 22, figs. 1-5, Pl, 23, figs. 1 and 2, 
 
564 
 
 Loc. Corporation Quarry, Maryborough (R. L. Jack ; G. Sweet—Colln. Sweet, 
 Melbourne; 7. W. H. David—Colln. David, Sydney). Occurs also in the Rolling 
 Downs Beds. 
 
 MAccoyveLLa REFLECTA, Moore, sp. 
 
 Pl. 23, figs. 8-7 and 10; ? figs. 1 and 2. 
 
 Avicula reflecta, Moore, Quart. Journ, Geol. Soc., 1870, xxvi., p. 246, t. 12, f. 1. 
 »  Barklyi, var. reflecta, Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. 2, p. 240, t. 12, 
 figs. 4-6, 
 
 Obs. This species is described under the head of “ Rolling Downs,” to which 
 the Reader is referred.* It has been found in the Desert Sandstone at the following 
 locality :— 
 
 Loc. Isis River, near Maryborough and Bundaberg Road (W. H. Rands). 
 Occurs also in the Rolling Downs Beds. 
 
 Maccoyetta ? susstriata, Moore, sp. 
 
 Pl. 23, figs. 8 and 9. 
 Avicula substriata, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 247, t. 11, f. 6. 
 
 Obs. As in the case of the other species of Maccoyella, this is described amongst 
 the Rolling Downs Mollusca.t The shells figured (Pl. 23, figs. 8 and 9) are believed 
 to appertain to the present species. The reference is chiefly made on account of the 
 extended posterior wing, but this is accompanied by a peculiar elevation of the hinge or 
 dorsal margin at its outward termination. The specimen is in a poor state of preserva- 
 tion, so that a definite opinion may be for the present held over. 
 
 Both figs. 8 and 9 occur in close contiguity on the same piece of matrix, and 
 are probably the right and left valves of the same species. They are but casts. Fig. 9 
 is a convex valye, and more or less oblique, bearing thirteen or more strong ribs. 
 The cardinal margin is long, and produced upwards, forming with the posterior end 
 a high elevated wing. The whole length of the cardinal margin is bordered by a 
 small longitudinally grooved area, not shown in the figure. The subject of fig. 8 
 is a flatter valve than fig 9, with finer and much more numerous ribs, and in addition 
 interpolated riblets, with the interspaces cross-striated. 
 
 Loc. Maryborough (&. LZ. Jack). Occurs also in the Rolling Downs Beds. 
 
 MaccoyveLia ? uMBoNALIS, Moore, sp. 
 Pl, 23, fig. 4. 
 
 Avicula umbonalis, Moore, Quart. Journ. Geol. Soc., 1870, xxvi., p. 246, t. 12, figs. 2 and 3. 
 
 Obs. This species is fully described under the head of “ Rolling Downs,” to 
 which the Reader is referred. t 
 
 I have not seen a perfect specimen of this species, but Mr. Rands has collected 
 a large bivalve at Maryborough which has some resemblance to Moore’s figure. It is 
 transversely ovate, with an obtuse umbo, and a sharp, incurved beak. A large number 
 of radiating ribs were present, some being larger and more determinate than the others. 
 
 Loc. and Horizon. Corporation Quarries, Maryborough (W. H. Rands; G. 
 Sweet—Colln. Sweet, Melbourne); Wharf Railway, Maryborough (W. H. Rands). 
 Occurs also in the Rolling Downs Beds. 
 
 
 
 * See p. 457, Pl. 23, figs. 1, 2, 3-7, and 10. 
 + See p. 459, Pl. 22, fig. 10. 
 t See p. 458, Pl. 22, figs. 6 and 7, 
 
565 
 
 Order—ARCACEA, 
 Family—ARCIDA. 
 
 Genus—CUCULLAA, Lamarck, 1801. 
 (Syst. Anim. sans Vertéb., p. 116.) 
 
 CucuLLzZA Ropusta, Htheridge, Pl. 26, figs. 1 and 4. 
 Cucullea robusta, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 340, t. 20, f. 1. 
 Ap costata, Etheridge, Ibid., t. 20, f. 2. 
 
 Sp. Char. Shell trapeziform or rhomboidal and nearly equilateral; body of the 
 valves very convex and inflated; dorsal margin straight, long; area wide and flat ; 
 posterior teeth three or four, horizontal crests of the teeth and bottoms of the sockets 
 denticulated ; ventral margin rounded, closed, the interior wide and flattened; anterior 
 and posterior ends truncated ; umbones large, gibbous, distant, and incurved ; pallial 
 fine straight; coste or ribs thirteen to twenty-four in number, equal, sharp, composed of 
 from three to five subordinate ribs, the posterior end apparently devoid of ribs; inter- 
 spaces wide, filled with very fine riblets parallel to the principal coste. 
 
 Obs. It is very questionable if two species exist at Maryborough, where these 
 shells appear to be moderately common. I have therefore combined both for the present 
 under one name. 
 
 The ribs, or costw, become wider apart towards the extremities of the valves, and 
 are sharp with wide interspaces. The latter are filled with very fine riblets, and the 
 whole surface is well cancellated by sub-imbricating frills. The usual number of 
 principal coste is thirteen, three on the anterior end and the remainder confined to the 
 body of the shell, the posterior end being apparently devoid of them, or at any rate 
 with the cost very faintly developed. Between each pair are four or five smaller or 
 secondary coste, besides the five lines previously mentioned. 
 
 Cucullea virgata, J. de C. Sby.,* from the “ Upper Secondary” Formation of 
 Cutch, is remarkably like C. robusta, both in shape and ornament. 
 
 Loc. Maryborough (The late R. Daintree); Corporation Quarry, Maryborough 
 (W. H. Rands; Messrs. T. W. EB. David and G. Sweet—Collns. David and Sweet). 
 
 Family —NUCULID®. 
 
 Genus—NUCULA, Lamarck, 1799. 
 (Prodrome—Meém., Soc, Hist, Nat. Paris, 1799, p. 87.) 
 
 Nucvura quaprata, Etheridge, Pl. 26, figs. 8 and 9. 
 Nucula quadrata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 341, t. 19, f. 5, t. 20, f. 3, 
 
 Sp. Char. Shell quadrate and tumid, umbones anterior, and anterior side short 
 and vertical; posterior side much elongated and sharply rounded; teeth on posterior 
 side large and numerous; those on anterior side few (seven or eight) and smaller ; 
 posterior dorsal margin flat. (Ztheridge.) 
 
 Obs. This and the following species appear to be unusually large for Cretaceous 
 forms. The muscular scars and pallial line are very strongly marked in the cast. _ In 
 one of Mr. Etheridge’s original figures of this species the scars of the retractor (?) 
 muscles, usually met with on the visceral region of the interior surface of Nucule, are 
 exceedingly developed, and give to the surface of the cast quite a pock-marked 
 appearance. It isa rather thick, heavy species, with fifteen or sixteen posterior, very 
 large hinge-teeth. 
 
 
 
 
 
 * Trans. Geol. Soc., 2nd Ser., v., Expl. t. 22, t, 22, f. 1. 
 
566 
 
 Loe. Maryborough (The late R. Daintree; the Hon. A. C. Gregory; Messrs. 
 T. W. E. David and G. Sweet—Collns. David and Sweet). Occurs also in the Rolling 
 Downs Beds. 
 
 Nucuta @igantea, Htheridge, Pl. 26, figs. 6 and 7. 
 Nucula gigantea, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 341, t. 20, f. 4. 
 
 Sp. Char. Shell ovately oblong; dorsal margin nearly horizontal; ventral 
 margin nearly semi-circular; umbones placed very anteriorly and nearly straight; hinge- 
 teeth thirteen or fourteen, on posterior side, and five or six on anterior side of umbo. 
 (Ltheridge.) 
 
 Obs. The ligamentary pit in this species is large and spoon-shaped, and directed 
 towards the posterior end. One specimen examined possessed sixteen teeth on the 
 posterior hinge, and another from Port Curtis only ten, but this may depend on 
 preservation. ‘The exterior was ornamented with fine concentric lines. 
 
 Loc. Maryborough (The late R. Daintree; Messrs. T. W. EB. David and G. 
 Sweet—Collns. David and Sweet) ; near Mullet Creek, twelve miles south of Rosedale 
 Station, Port Curtis (W. H. Rands). 
 
 Genus—NUCULANA, Link, 1807. 
 
 (Beschr. Natur. Sammi. Rostok, iii., p. 155.) 
 
 Nvucurana (? Youp1s) Ranpst, sp. nov., Pl. 26, fig. 10. 
 
 Sp. Char. Shell elongately ovate, rather tumid, moderately large, rostrate 
 posteriorly. Cardinal margin or hinge-line somewhat convex in front, excavated or 
 concave behind, with about fourteen teeth both on the anterior and posterior sides. 
 Anterior end rather produced; anterior and ventral margins rounded. Posterior end 
 bluntly rostrate, curved upwards. Umbones sub-central. 
 
 Obs. The surface markings and the pallial line are not visible, but I believe the 
 species is referable either to Nuculana or Yoldia. It is allied to such as Leda protexta, 
 Gabb,* and Yoldia seaphuloidea, Stoliezka,} more particularly the latter, but differs in 
 size and in having a more acute rostrum. 
 
 The species is named in honour of Mr. W. H. Rands, Assistant Government 
 Geologist of Queensland. 
 
 Loc. Isis River, near Bundaberg Road, Wide Bay (W. H. Rands). 
 
 Genus—ADRAWNA, fl. and A. Adams, 1858. 
 (Gen. Recent Moll., 11., Pt. 33, p. 547.) 
 
 ADRANA ELONGATA, Ltheridge, sp., Pl. 33, fig. 8. 
 Leda clonyata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 341, t. 20, f. 5. 
 
 Sp. Char. Shell elongated, length nearly double the height; umbones nearly 
 central, nearer anterior than posterior margin; teeth very numerous on both sides of 
 umbo, anterior twelve or thirteen, posterior fifteen. (Htheridge.) 
 
 Obs. In form this species seems to approach much nearer to H. and A. Adams’ 
 genus Adrana than either to Leda or Yoldia. The resemblance to Leda scapha, d’Orb., 
 does not appear to be so apparent, as stated by Mr. Etheridge. As regards Yoldia 
 scaphuloidea, Stol., of the Arrialoor Group of India, the likeness is greater, but the two 
 shells are clearly distinct. When perfect, the anterior margin is regularly rounded, and 
 
 * Pal. California, 1864, i., p. 199, t. 26, f. 185. 
 + Pal. Indica (Cret. Fauna), iii., 1871, Fas. 5-8, p. 324, t. 17, £. 11 and 12. 
 }Non Adrana, Loew, 1878, a genus of Diptera, nec Adrania, Stal, 1863, a genus of Hemiptera. 
 
567 
 
 tolerably deep from the dorsal to the ventral. There is no definite evidence of the 
 valves gaping, although some appearance of this does exist at the posterior end of one 
 specimen. It was evidently a very much compressed species. An example collected 
 by Prof. T. W. E. David measures one and a-half inches in length. 
 
 Loc. Maryborough (Zhe late R. Daintree; T. W. EB. David—Colln. David, 
 Sydney). 
 
 Family—TRIGONIDA. 
 
 Genus—TRIGONIA, Bruquiére, 1789. 
 (Encyel. Méthod. i., Pl. 14.) 
 
 TriIgonra Nasuta, Ltheridge. 
 Trigonia nasuta, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 339, t. 19, f. 2, 2a. 
 
 Sp. Char. Shell triangular or deltoid, much produced or elongated at the 
 posterior end; anterior side truncated; umbones prominent and thick; hinge area and 
 teeth not preserved, save a few on the posterior area. (Ltheridge.) 
 
 ‘Obs. We possess only the cast of this shell, and had it been found in the 
 Cretaceous rocks of Britain we should have allied it to Trigonia aleformis, Park., or 
 T. caudata, Ag., but from the umbo to the ventral margin it is much higher or deeper 
 than either of the two forms referred to. I am inclined to believe that the concentric 
 folds or ribs supported tubercles upon them, as in Vrigonia scabra and T. caudata. 
 I unhesitatingly refer it to the Cretaceous deposits, and it belongs to a type not known 
 in the Jurassic rocks. 7. sancte-crucis, Pictet and Camp., much resembles this shell; and 
 again, Mr. C. L. Griesbach describes a Trigonia, from the Umtafuna River, Natal, 
 which has an elongated posterior end, and, in general shape and deltoid form, is much 
 like our shell. (2theridge.) 
 
 The folds distributed over the umbonal region in Mr. Etheridge’s figure are shown, 
 on the internal cast of a left valve obtained by Prof. IT. W. E. David, to occur generally 
 over the whole valve, except on the posterior slope. ‘They are wide and flat. 
 
 Loc. Maryborough (Lhe late R. Daintree; TL. W. E. David—Colln. David, 
 Sydney). 
 
 TRIGONIA, sp. ind. (a.), Pl. 26, fig. 5. 
 
 Sp. Char. Cast subovately elongate, subconvex, but not inflated; anterior side 
 rounded from the umbones downwards, and but little produced; posterior side pro- 
 duced into an obtuse, somewhat flattened, nasiform extension, witha straight oblique 
 margin; ventral margin rounded, extended, without apparent undulation or excavation 
 posteriorly ; hinge-line concave, sloping towards the posterior end; umbones acute, little 
 incurved, nearly vertical to the longer axis of the shell; area narrow and elongate, 
 bounded by a sub-acute ridge from the umbones, which gradually dies out; escutcheon 
 not preserved; dental sockets oblique, divergent, the anterior tear-shaped and long, the 
 posterior thin ; flanks of the cast but little convex, whilst the posterior end immediately 
 below the bounding carina of the area bears a depression or groove. 
 
 Obs. An exceedingly well-preserved cast, which appears to differ from any of 
 the hitherto described Australian Trigonias, but is probably nearest to 7. mesembria, 
 Woods. It differs entirely in shape from Z. lineata, Moore, and is not sufficiently 
 pointed at the posterior end for 7. nasuta, Etheridge. In many points this cast agrees 
 with Trigonia conocardiiformis, Krauss,* from the Cretaceous rocks of South Africa, but is 
 
 
 
 * Nova Acta Acad, Cees, Leop.—Carol. Nat. Curio., 1850, xxii., Pars. 2., p. 454., t. 49, f. 1. 
 
 
 

 
 568 
 
 by no means so massive a shell, and some of the internal characters are different ; still, 
 it is undoubtedly closely allied to Krauss’ species. It doesnot in any way agree with the 
 other South African Cretaceous shell, Zrigonia Shepstonei, Griesbach.* 
 
 I think it quite likely that the present shell may be an elongated variety of 
 LP. mesembria, Ten. Woods, but as the figure of this species represents an individual with 
 the shell on, and the present fossil is only a cast, it is difficult to compare them. On 
 the difficulty of dealing with Trigonia casts, the late Dr. Lycett made the following 
 remarks, which are very applicable to these Australian forms. He said :—‘“ It rarely 
 happens that any. of the external ornaments are visible upon them; and even under the 
 most favourable conditions the impressions of these ornaments are only faintly and 
 insufficiently shown, so that by means of these alone the external aspect even of a 
 single species could never be fully ascertained, and even when both the mould and test 
 have been obtained it is not in every instance that the mould can with certainty be dis- 
 criminated from those of other allied species. The practice of authors, therefore, who 
 have described supposed new species even partially, and have named them from internal 
 moulds alone, is objectionable, as tending to create doubt and hesitation in the minds of 
 students, and encumbering the list of species with things which for all practical purposes 
 are little more then mere names.” 
 
 Loc. Maryborough (Hon. A. O. Gregory). 
 
 Family—CY PRINID&. 
 
 Genus—CYPRINA, Lamarck, 1818. 
 (Hist. Anim. sans. Vert¢b., v.) 
 
 Cyrprina CrarKet, Moore, Pl. 27, fig. 9; ? Pl. 26, figs. 18 and 19. 
 (For description see under *‘ Rolling Downs,” p. 474.) 
 
 Obs. This shell appears to have attained considerable dimensions in the 
 Australian Cretaceous seas, being much larger than the Cyprina planata of the Lower 
 Tertiaries of Britain and France. In form and habit C. erpansa is closely allied to C. 
 planata, possessing also the compressed ventral border, deep lunule, and expanded 
 anterior or pedi-lateral margin. (Ltheridge.) 
 
 C. expansa is a-very characteristic species of the North Queensland Cretaceous 
 deposits. In the Maryborough Beds it has invariably been met with in casts, but in 
 the nodular limestone of the Walsh River portions of the shell are usually attached to 
 the specimens. In some individuals the anterior side is longer, and the dorsal margin 
 very much more oblique, than represented in Mr. Etheridge’s figure. The umbones are 
 much incurved, and the lunule deep. The anterior end rather compressed and flattened 
 towards the margins. The pallial line is strongly marked, but the sinus is not deep. The 
 shell, where preserved, is thick and concentrically corrugated, with fine intervening 
 concentric lines. 
 
 Loc. and Horizon. Maryborough (Lhe late R. Daintree; T. W. HB. David— 
 Colln. David, Sydney; G. Sweet—Colln. Sweet, Melbourne). 
 
 In connection with this genus may be mentioned a shell (Pl. 27, Fig. 1) 
 figured + by Mr. Etheridge without name. The following is his description :—‘ Shell 
 apparently smooth, semicircular, nearly equilateral, equivalve ; umbones central, slightly 
 acute and anterior ; posterior and ventral margins equally rounded and smooth; hinge-~ 
 line straight, rounded at the angles, giving the shell an almost circular appearance.” 
 
 
 
 
 
 * Quart. Journ. Geol. Soc., 1871, xxvii., t. 3, f. 11. 
 + Ibid., 1872, xxviii, p. 389, t. 19, f. 4. 
 
569 
 
 “Obs. It is to be regretted that we have not a particle of the original shell 
 wherewith to recognise the nature of the markings, or even the ventral margin to aid 
 us in determining whether the inner edge was erenulated or plain; externally the shell 
 appears to have been smooth or delicately concentrically marked. The cast of the 
 hinge-line is such as to prevent our determining any teeth below the junction of the 
 two valves. 
 
 “In outward form this shell much resembles Lweina (Codakia) pererassa, Stol., 
 from the Arrialoor Group (India) ; and the shell is nearly equal in length to that of 
 this species, but not so high. The pallial line appears to be simple; and the muscular 
 impressions resemble those of Pectunculus. Some Axinea from the Indian Cretaceous 
 rocks, but for their size, would very closely resemble this shell. We possess one 
 specimen only, and that a cast of one valve. 
 
 Three similar casts have come under my own observation (Pl. 27, fig. 1), but I 
 am in no way better prepared to offer any definite suggestion as to their generic affinity 
 than was Mr. Etheridge. Cardinal and lateral teeth were undoubtedly present, so that 
 the supposed resembiance to Awinea (Pectunculus) may be at once dismissed. The 
 hinge characters, however, are too ill-preserved to warrant us in a complete generic, 
 reference, but, in all probability, these shells belong either to the Cyprinide or Luci- 
 nide. Fora true Cyprina, the umbones are too central, although slightly on the 
 anterior side; whilst the absence of crenulations along the ventral interior of the valves 
 separates them at once from that section of Codakia referred to by Mr. Etheridge. 
 
 Prof. K. Martin has described a large shell, having much the appearance of our 
 fossils, but with the shelly matter preserved, from the Tertiary Beds of Java. He 
 provisionally refers it to Lucina.* 
 
 Prof. J. D. Dana, again, has figured a similar form, referred to the same genus, 
 from the Tertiary series of Oregon, under the name of Lucina acutilineata.t The 
 outline corresponds well with our shell. 
 
 The almost central beaks, and nearly round outline, with an apparently indefinite 
 or smooth surface ornament, are features of too marked a character to be easily passed 
 over. The posterior muscular scar was large, deep, and round-oval, and the pallial sinus 
 wide and open, and it is not impossible that we may here have the foreshadowing of a 
 new genus. In two of the specimens one of the valves has been thrust upwards, 
 producing an apparent inequality of the valves, but in the third they are normal. 
 
 Loc. Maryborough (The late R. Daintree). 
 
 Order—LUCINACEA. 
 Family—LU CINID. 
 
 Genus—UNICARDIUM, @ Orbigny, 1850. 
 (Prod. Pal. Strat., i, p. 218.) 
 
 Unicarpium ? ETHERIDGEI, sp. nov., Pl. 27, fig. 1. 
 Genus 7, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 339, t. 19, f. 4. 
 
 Sp. Char. Shell large, more or less semicircular, if anything slightly oval, the 
 transverse measurement being slightly the greater, nearly equilateral, convex, and 
 inflated in the umbonal region. Dorsal margin nearly straight, rounded at the lateral 
 angles; anterior and ventral margins rounded, but the posterior slightly produced. 
 
 
 
 * Sammlungen Geol. Reichs Mus. in Leiden, 1888, i., No. 5, Heft 4, t. 13, f. 43. 
 + Geology, Wilkes’ U. S. Explor. Exped., 1849, x., Atlas, t. 18, f. 2, 
 
570 
 
 Umbones large, incurved, slightly anterior. Cardinal teeth large, apparently one in 
 each valve; the dorsal margin thickened internally on the posterior side, and assuming 
 a rather lateral, tooth-like appearance. Adductor muscular scars well developed, 
 especially the posterior, which is deeply excavated on the outer side. Surface with wide 
 concentric lamine, and intermediate finer lines of growth. 
 
 Obs. The reference to Unicardium is made provisionally, as the casts of this 
 shell have long puzzled me, as did those in Daintree’s Collection perplex Mr. Etheridge. 
 It always occurs as internal casts and from the one locality, the almost equilateral form 
 and central beaks being among its chief peculiarities. 
 
 The pallial line is simple, although in our illustration (Pl. 27, fig. 1) it appears 
 sinuated, but this only arises from a fracture, all other specimens having presented a 
 perfectly continuous line. 
 
 Named in honour of my Father, Mr. Robert Etheridge, F'.R.S. 
 
 Loe. and Horizon. Corporation Quarry, Maryborough (Zhe late R. Daintree, 
 and R. L. Jack; G. Sweet—Colln. Sweet, Melbourne). 
 
 Order—TELLINACEA, 
 Family—TELLINID. 
 
 Genus—PALAHOMGRA, Stoliczka, 1870. 
 (Pal. Indica (Cret. Fauna), 1870, iii., Fasc., 1-4, p.116.) 
 
 PALHOMERA MARIEBURIENSIS, Ltheridge, sp. 
 Telling Maricburiensis, Utheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 341, t. 20, f. 6 and 6a. 
 
 Sp. Char. Shell compressed, transversely elongated, nearly equilateral, acutely 
 rounded anteriorly; posterior margin slightly truncated ; lines of growth strongly 
 marked and band-like; these concentric bands are broad and of equal width, 
 (Ltheridge.) 
 
 Obs. In many respects this shell resembles Tellina (Paleomera) inconspicua, 
 Forbes, from Trichinopoly ; but the band-like markings, if in the external shell, which 
 they appear to be, remove it from that species; in form, size, and habit, however, it 
 closely approaches the latter. (Etheridge.) 
 
 The distant concentric depressions appear to be a very characteristic feature in 
 this species. 
 
 Loc. Maryborough (The late R. Daintree ; G. Sweet—Colln. Sweet, Melbourne). 
 
 PALHOM@RA? sp. ind., Pl. 26, fig. 17. 
 Tellina sp., Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 341, t. 20, f. 7. 
 
 Obs. This species is less elongated and more deltoid in form than P. marieburiensis, 
 and apparently possessed a smooth shell instead of the banded structure of that 
 species; the anterior side is obtusely rounded, and the posterior more acute. 
 (Ktheridge.) 
 
 A small form resembling this occurs in the Walsh River nodules, but the 
 specimens appear to have an inflection in the posterior ventral margin. 
 
 Loe. Maryborough (Lhe late R. Daintree). 
 
 Genus—GLYOIMERIS (Klein), Lamarck, 1799. 
 
 Glycimeris (Klein), Lamarck, Mém. Soc. Hist. Nat. Paris, 1799, p. 83 [non Lamarck, 1801, Syst. Anim. 
 sans. Verbéb., p. 126=Cyrtodaria, Daudin]. 
 Panopea, Ménard de la Groye, Ann. Mus. Hist. Nat. Paris, 1807, ix., p. 135 
 Obs. Glycimeris is here used as originally proposed by Klein, and adopted in 
 his earlier writings by Lamarck, who was a binomial Author. As employed by the 
 
571 
 
 latter in his “Systtme’’ it is equal to Crytodaria, Daudin. In this sense Panopea, Ménard, 
 simply becomes a synonym. The two species described by Mr. Moore it is almost 
 impossible to recognise, the figures are so indefinite and badly executed. They may be 
 here described under other names, but in such cases this cannot be avoided. 
 
 GLYCIMERIS suLcaTa, Ltheridge, sp., Pl. 17, fig. 18. 
 Panopea sulcata, Etheridge, Quart. Journ. Geol. Soc., 1872, xxviii., p. 342, t. 21, f. 2 and 2a. 
 
 Sp. Char. Shell oblong, transversely or ovately elongated, thin, with many 
 concentric, deeply sulcated plications or furrows ; umbones pointed, anterior side much 
 rounded, posterior side acute. (Ltheridge.) 
 
 Obs. This shell resembles P. orientalis, Forbes *; but the concentric sulcations 
 are fewer and coarser, the posterior margin is more acute, and the umbones slightly 
 more central. It also much resembles P. Prevost, D’Orb.,f but our shell is more 
 coarsely plicated than either of the abovenamed species. (Ztheridge.) 
 
 Crushed examples appear to be plentiful in the Maryborough Beds. What 
 appears to be a short variety also exists with few and exceedingly coarse concentric 
 ribs. Individuals of G. sulcata vary greatly in appearance, both as regards the 
 coarseness of the furrows on the surface, and the marginal outline of the anterior end. 
 Impressions of the thickened hinge-margin are usually well displayed on these casts. 
 The posterior end gaped but little. 
 
 This is certainly distinct from G. rugosa, Moore, judging from the form and 
 concentric, corrugated lamine, but it may be allied to Moore’s Mya Maccoyi. The later 
 Author says that the anterior margin of his species is truncated and angular, and so is 
 that of G. swleata. If the former is also a somewhat long and narrow shell, resembling 
 a specimen in Prof. Tate’s South Australian Collection, the resemblance is intensified. 
 Specimens of this species are always so crushed that it is difficult to say what the precise 
 structure of the dorsal margin was—whether a ligamental fulcrum existed as in 
 Glycimeris, or a cartilage process as in Iya. 
 
 The variety is short and obtuse, and is distinguished by having the length much 
 less in proportion to the width (Pl. 17, fig. 18) than the species proper. It may 
 perhaps represent a distinet species. 
 
 Loc. Maryborough (The late R. Daintree) ; Corporation Quarry, Maryborough 
 (W. H. Rands ; and G. Sweet—Colln. Sweet, Melbourne). 
 
 GuycrmeriIs ruGosA, Doore, sp., Pl. 28, figs. 4 and 5, ? f. 6. 
 (For description see under ‘‘ Rolling Downs Beds,” p. 478.) 
 
 Loc. Prof. T. W. E. David has collected an internal cast in the Corporation 
 Quarry, Maryborough, which appears to be too large a shell for G. sulcata, Eth., and 
 may indicate the presence of the present species. 
 
 Occurs algo in the Rolling Downs Beds. 
 
 Genus—CEROMY A, L. Agassiz, 1842. 
 (Etudes crit. Moll. Foss. 2e., p. 25.) 
 CEROMYA? sp. ind., Pl. 26, fig. 20. 
 
 Obs. This ill-preserved, although stratigraphically important, cast is pro- 
 visionally referred to the present genus. One valve is much crushed, but the other is 
 
 
 
 * Trans. Geol. Soc., 2nd. Ser., vii., p. 189, t. 17, f. 4. 
 + Pal. Franc. Terr. Crét., 1843, iii., p. 354, t. 356, f. 3 and 4. 
 
572 
 
 fairly intact; but the whole of the test has been removed. It possesses the oblong 
 outline of several species of Ceromya, and was similarly inflated about the umbones. 
 The dorsal margin is fairly straight ; the umbones much inrolled, overhanging a large 
 false lunule. The exterior was concentrically and broadly laminated as in several 
 Ceromye. The specimen is five and a-half inches long by three and three-quarter 
 inches high. Its relation to the genus will be apparent if such species as Ceromya 
 excentrica, Voltz, sp., are compared with it. 
 
 Ceromya is chiefly an Oolitic genus, but Agassiz has described species from the 
 Neocomian. 
 
 Loc. Maryborough (Zhe Hon. A. C. Gregory). 
 
 Family—MACTRID. 
 
 Genus—LUTRARIA, Lamarck, 1799. 
 (Prodrome—Mém. Soc. Hist. Nat. Paris, 1799, p. 85.) 
 
 Lvurraris, sp. ind. 
 
 Obs. A very indifferent cast may perhaps be referable to this genus. On the 
 other hand it is not unlike some forms of Siliqua or Oultellus. The specimen is two 
 inches long, and broken posteriorly. It is a cast of the exterior. 
 
 Loc. Maryborough (The late R. Daintree). 
 
 Order—-PHOLADACEA, 
 Family—PHOLADID. 
 
 Genus—TEREDO, Linneus, 1758, 
 (Syst. Nat., Edit. x.) 
 
 TEREDO, sp. ind., Pl. 43, figs. 11 and 12. 
 
 Obs. Portions of tubes resembling those of Zeredo, especially the Cretaceous 
 Teredo amphisbena, occur in the siliceous rock of the Croydon Gold Field. The valves 
 of the shell are unknown. The tube is moderately tortuous and curved, two and 
 a-quarter inches long, and seven-sixteenths of an inch in diameter. The test is thick. 
 (Pl. 43, fig. 11.) 
 
 In addition to the species named there is also a resemblance to 7. partita, 
 Stoliczka,* and 7. Reguienianus, Math.,+ of the French Chloritic Chalk, but our form 
 is rather larger than the latter. It corresponds with species of this description better 
 than it does with the smaller forms of the Oolitic rocks. 
 
 A very interesting specimen (Pl. 48, fig. 12) was given to me by the late Rev. 
 J. E. T. Woods, consisting of a number of shelly tubes of Zeredo, most of them straight 
 and parallel, but one or two curved, and preserved in a drab limestone. The longest is 
 over two inches, with a diameter of three-quarters of an inch, but the average diameter 
 is a quarter of an inch. Many of these tubes are seen in section, and at the larger end 
 of one of them are two disjointed and displaced valves, probably those of the species. 
 The specimens closely resemble Zeredo crassula, Stol.,t and the section of the valves 
 would agree intimately with those of our fossils. 
 
 
 
 * Pal. Indica (Cret. Fauna), 1871, iii., t. 1, f. 1. 
 + D’Orbigny, Pal. Franc. Terr. Crét., iii., p. 303, t. 348, f. 3-6. 
 + Pal. Indica (Cret Fauna), 1871, iii., t. 1, f. 2 @ and 0. 
 
573 
 
 Teredo-bored wood also occurs in the Rolling Downs Series, Mr. G. Sweet having 
 obtained such from the Walsh River, and at Hughenden, the borings being from ten to 
 fifteen millimetres wide. 
 
 Loc. True Blue Hill, Croydon (W. Samwell). 
 
 Class—GASTEROPODA. 
 Order—PULMONATA. 
 Family—SIPHONARIID A. 
 
 Genus—SIPHONARIA, G. B. Sowerby, 1824. 
 (Genera of Shells i., Pl. 143.) 
 
 SrPHONARIA SAMWELLI, sp. nov., Pl. 42, fig. 9. 
 
 Sp. Char. Shell patelloid, depressed conical; anterior margin expanded on the 
 left side; posterior contracted; apex recurved and much depressed. Surface with a 
 large number of radiating costs, not all equal in size, but about twelve stronger than 
 the others proceeding direct from the apex; the intermediate and smaller coste# proceed 
 from the margin for two-thirds the distance between the latter and the apex, but do not 
 reach the last-named ; the whole are crossed by very wavy and sub-imbricating ridges, 
 which become more numerous and delicate as the periphery is approached. 
 
 Obs. This shell is known under the condition of impressions of the exterior. 
 The unsymmetrical outline suggested to Mr. J. Brazier, who examined the specimens, 
 the genus Siphonaria as a more fitting resting-place than Patella. The interior has not 
 been observed. 
 
 Of Stiphonaria, Mr. G. B. Sowerby remarked: “ Its lateral canal, and the vertex 
 being obliquely turned backwards, may be considered as its principal distinctive 
 characters, separating it not only from Patella, but from Hmarginula, whose canal is 
 anterior and vertex posterior.” 
 
 The nearest fossil ally I have seen is Patella caperata, Tate, from the Uitenhage 
 Series (Jurassic) of South Africa. This is, however, a Siphonaria in all probability, as 
 the “ periphery is irregular, and slightly sinuated.” 
 
 The present species is named in compliment to Mr. W. Samwell, late Goldfield 
 Warden, who collected extensively at Croydon. 
 
 Loe. True Blue Hill, Croydon (W. Samwell). 
 
 
 
 PECTINIBRANCHIATA. 
 Family—NATICIDZ. 
 
 Genus—NATICA, Adanson, 1757. 
 (Hist. Nat. Sénégal, Coquilles, p. 172.) 
 
 Order 
 
 Nartica VARIABILIS, Moore, Pl. 31, figs. 2 and 3. 
 (For synonymy and description, see p, 485.) 
 
 Loc. Maryborough (The late R. Daintree), Occurs also in the Rolling 
 Downs Beds. 
 
574 
 Class—CEPHALOPODA. 
 
 Order—DIBRANCHIATA. 
 Family—BELEMNITID. 
 
 Genus—BELEMNITES (G4. Agricola), D’ Orb., 1840. 
 (Pal. Frane. Terr. Crét., 1840, i., p. 37.) 
 
 Obs. Mr. Rands notes * the presence of “numerous casts of Belemnites” in the 
 Maryborough Desert Sandstone in a quarry “just a couple of hundred yards on the 
 Maryborough side of the Copenhagen Bend” of the Mary River. I have not seen any 
 of these casts, but Prof. T. W. E. David obtained a portion of the highly altered rock 
 at the Corporation Quarry, Maryborough, with an elongated cavity, which may be either 
 that left by the decomposition of a Belemnite or a Dentalium. 
 
 Another specimen in Mr. Sweet’s Collection is an elongated hollow, in the proximal 
 end of which reposes a portion of a phragmacone. The distal extremity bears two 
 lateral ridges indicating the lateral grooves, and the distal outline gradually swells out 
 with an oval section resulting in a form much resembling Belemnites Canhami, Tate, to 
 which it is probably allied, although the apex of the guard is too pointed to be that 
 species. 
 
 EK. 
 
 a 
 * Report on the Burrum Coal Field. Brisbane; by Authority 1886 ~ 
 
CHAPTER XXXYV. 
 
 TERTIARY. 
 
 LOWER (MIOCENE?) AND UPPER (PLIOCENE?) VOLCANIC ROCKS AND 
 DRIFTS. 
 
 RUSSELL RIVER AND MULGRAVE GOLD FIELDS, MOUNT MORGAN GOLD MINE. 
 
 The presence of Tertiary rocks in Queensland is rather inferred than proved. 
 
 To begin with, it is in the highest degree unlikely that this epoch passed over in 
 Queensland without any deposition of either fresh-water or marine strata, such as 
 exist in all the neighbourning colonies. The absence, so far as we know for certain, of 
 Tertiary marine strata may be due to the fact that the elevation which took place after 
 the deposition of the Upper Cretaceous (Desert Sandstone) rocks placed the whole of 
 Queensland above the reach of the ocean during Tertiary times. But in that case we 
 should expect a widespread accumulation of fresh-water deposits. 
 
 Daintree, indeed, who describes the’ Desert Sandstone as “ without doubt the 
 most recent, widely-spread stratified deposit developed in Queensland,” and correctly 
 observed that it lies unconformably on the Cretaceous Rocks of the “ Rolling Downs,” 
 classed the Desert Sandstone as “ Cainozoic,” adding “all that can be asserted is that 
 its horizon is above and unconformable to the Cretaceous Series of the Flinders.” As 
 will be seen in the Chapter relating to the Desert Sandstone, that Formation must be 
 regarded as Upper Cretaceous, the idea of its “ Cainozoic”’ age being no longer tenable. 
 
 There is reason to believe that the Tertiary epoch was marked by intense 
 voleanic activity, accompanying or following extensive movements of elevation. It 
 may be well at the outset to glance at the history of volcanic activity in the other 
 colonies in Tertiary times before considering whether Queensland affords any evidence 
 of similar activity. 
 
 In Victoria, according to Mr. Reginald A. F. Murray, Government Geologist,* 
 the Eocene of Europe has no Victorian representative. “ The Victorian Lower Tertiary 
 beds, which the term Oligocene has been employed to designate, really belong to the upper- 
 most portion of the Lower Tertiary group, arid appear to occupy an intermediate 
 position between the Eocene and Miocene.” These consist exclusively of marine 
 deposits. 
 
 The Middle Tertiary (Miocene) is extensively developed in Victoria. It 
 comprises “ deposits due to marine, lacustrine, and fluviatile agencies, and also the rocks 
 of igneous origin, classed as Older Volcanic, which appear to be the youngest of the 
 group, and to form the division between beds of Middle Tertiary and Miocene and 
 those of Upper Tertiary or Pliocene age.” 
 
 “The Older Volcanic rocks are the latest products, and mark distinctly the close 
 of the Middle Tertiary or Miocene era. There do occur, occasionally, thin volcanic 
 layers, interstratified with the Miocene sedimentary beds, showing that vulcanicity was 
 not altogether dormant during the formation of the latter, but the greatest volcanic 
 activity evidently took place at the close of the period. Where undecomposed, the 
 Older Voleanic basalts are usually dark, dense, and solid, of a polygonally jointed and 
 
 
 
 * Geology and Physical Geography of Victoria. Melbourne: by Authority : 1887. 
 
576 
 
 sometimes distinctly columnar structure, and composed chiefly of augite, labradorite, 
 olivine, and specular iron. They are, however, as a rule, either wholly or partly decom- 
 posed. In the former condition they consist of red, yellow, purple, brown, and nearly 
 white amygdaloidal clays, containing hard lumps of less decomposed rock showing 
 concentric structure; in the partly decomposed state, the rock exhibits in sections the 
 appearance of a conglomerate of such concentric masses in a clay matrix. 
 
 “Tn every locality throughout the Coiony where the Older Volcanic rocks are 
 at the surface, the soil immediately resting on or derived from them is of great fertility 
 and of exceptional value for agriculture. In the Neerim, Brandy Creek, and other 
 districts in Gippsland, the natural vegetation growing on such soil is of a most 
 luxuriant, sub-tropical character, forming a serious impediment to the labours of the 
 selectors, who, during late years, have eagerly taken up every available acre of such 
 land. 
 
 ‘The sources whence the Older Voleanic lava streams issued have not yet been 
 distinctly recognised ; no well-marked points of eruption, such as are common in the 
 Newer Volcanic districts, have been observed, and it would appear that the original 
 volcanic cones have been entirely removed by subsequent denudation, so that it would 
 only be in what are now narrow or small pipe-shaped dykes, easily passed over 
 unobserved, and probably far distant from where the Older Voleanic rocks remain in 
 considerable area, that we might look for the vents whence the flows were poured forth. 
 The original extent covered by Older Volcanic rocks was once very much greater 
 than now. ‘The areas we now see occupied by them are, for the most part, disconnected 
 vestiges of what were once long, continuous, and frequently also widespread sheets, 
 which have been cut into and through by subsequent denuding agencies, so that in many 
 places the Older Volcanic rocks, which, at the time they were poured forth as lavas, 
 flowed down and partly filled in the valleys of the period, are now the eappings of 
 ranges, owing to the erosion of still deeper valleys on either side. Enough still remains 
 to enable some conjectures to be formed as to the areas once occupied by the Older 
 Volcanic rocks. The conclusions arrived at will, however, be better understood after 
 the existing Older Volcanic areas have been described, and will, therefore, be included 
 in the general sketch history of the Tertiary period, given in a subsequent chapter. 
 
 “Older Volcanic rock occurs in patches, filling hollows in Miocene and other 
 older formations in the neighbourhood of the Moorabool River, near Maude, and in one 
 place as an intercalated band between marine Miocene beds; it also constitutes a 
 considerable area of the Bellarine distri¢t, south of Geelong Harbour. 
 
 “From between Ballan and Blackwood down to near Bacchus Marsh the Older 
 Volcanic rock occurs in a number of localities, especially on the Pentland Hills, where 
 some of the undecomposed basalt of this age is highly magnetic. 
 
 “From near Romsey down to Melbourne there are several exposures of this 
 rock in beds and banks of creeks that have cut their way down to it through newer 
 overlying formations. Near Flemington is an area consisting of Older Volcanic 
 decomposed basalt, which may be seen in natural section on the bank of theSaltwater River, 
 passing under Upper Tertiary ferruginous deposits, capped with basalt of Newer Volcanic 
 age. From Hoddle’s Creek, a branch of the Upper Yarra, a series of disconnected 
 patches, in some places underlaid by auriferous gravels, are traceable, in the direction 
 of Melbourne, as far as Lilydale. Other patches occur between the Yarra and the 
 Plenty, near the Kangaroo Ground. This formation occurs again at Berwick and 
 Cranbourne, and has been proved by boring operations to exist beneath some two 
 hundred feet of Upper Tertiary deposits near Frankston. Cape Schanck and portion 
 of the country between Western Port and Port Phillip, also Phillip Island and French 
 
577 
 
 Island, in Western Port Bay, consist of Older Volcanic rocks, in places undecomposed, 
 and consisting of hard, dark, dense basalt. This rock, more or less decomposed, occupies 
 a strip extending from Griffith’s Point along the east coast of Western Port Bay, and I 
 believe this to be portion of and continuous with the French Island and Phillip Island 
 layers, and to be united, beneath the Newer Tertiaries, with the Older Volcanic rocks 
 which occupy so extensive a tract in the Neerim and Buln Buln district. 
 
 “Large and small strips and patches are found between the Tanjil and La Trobe 
 Rivers, and in various portions of South Gippsland. A well-defined lead, covered by 
 two hundred feet of older basalt, has been proved to trend, from between Walhalla and 
 Mount Baw Baw, southward to the level country near Toongabbie. Very extensive 
 sheets of older basalt probably underlie parts of the low Upper Tertiary country of 
 Gippsland, as it may be seen sloping from the hilly country, and passing under the plains 
 at Haunted Hill, Toongabbie, Seaton, Glenmaggie, and also at many places on the south 
 side of the La Trobe Valley. The basalt of the Dargo and Bogong High Plains has 
 been classed as Older Volcanic, because it immediately overlies sedimentary beds 
 containing Miocene flora, and its lithological character also justifies this classification. 
 Here we find many hundreds of feet in thickness of lava, for the most part undecomposed, 
 and often highly magnetic, showing, in many places, columnar structure in a marked 
 degree. Portions of the plains where the rock is bare resemble a pavement of five- 
 sided blocks; while, on the slopes below the escarped edges of the plains, acres in 
 extent are covered with pentagonal columns of basalt like logs confusedly heaped 
 together. 
 
 “Similar outlers of basalt, but of less extent, occur at Connor’s Plain and 
 Fullarton’s, Spring Hill, both points on the Main Divide between the Gippsland and 
 Murray River basins ; also to the southward at Mount Useful and Mount Lookout, the 
 ranges between the Aberfeldy and the Thomson, and between the Thomson and the 
 Tyers Rivers. A very small outlier occurs on the east slope of Mount Matlock, and 
 other patches are found on the Southern Spur, between the sources of the Yarra and 
 those of the La Trobe. 
 
 “The general evidence obtained from observations of the Older Volcanic areas 
 points irresistibly to the conclusion that they are remnants of extensive lava-flows 
 which poured down the valleys of the Miocene period, partially filling in the basins and 
 covering the sedimentary deposits in them, and also spreading in wide layers over the beds 
 of the estuaries and inlets. Subsequent denudation has cut through and destroyed the con- 
 tinuity of these lava-flows; new channels have been excavated to lower levels than 
 the ancient ones, which they filled, and fresh accumulations have in many places over- 
 spread them.” 
 
 Under the head of Upper Tertiary, Mr. Murray says,* ‘ are included all aqueous 
 deposits marine or fluviatile, and associated lava-flows, younger than the Older Volcanic 
 and older than the Newest Voleanic rocks, which latter are taken as the latest products 
 of the Tertiary period; deposits newer than they being regarded as Post-Tertiary and 
 Recent.” 
 
 “The basalts, or anamesite and dolerite lavas, familarly known as ‘bluestone,’ 
 occur in sheets or strips of varyirg breadth overlying a large extent of the central 
 western portion of Victoria. The great plains of the Western district, from Geelong to 
 Hamilton, and from Colac to Ararat, are nearly wholly of voleanic origin, while most of 
 the ancient river-beds or leads trending north and south from the Main Divide are 
 more or less filled in and covered by lava-flows, which, though often confined between 
 elevated Silurian ridges near the hilly country, spread out and unite with the wide sheets 
 
 a i i 
 
 Loe. cit, p. 113. 
 
578 
 
 that constitute the plains. To the northward of Ballarat, portion of the Main Divide 
 itself is of voleanic formation, and a wide-sheet extending to the north, and finally dis- 
 appearing under the Post-Tertiary deposits of the Loddon, covers the system of deep leads 
 of Creswick, Clunes, and Daylesford, on their trend towards the Murray. At Ballarat 
 there are four, and in other places two or three, distinct layers of basalt covering the leads. 
 
 “The lowest overlie the deepest part of the gutters, and the next in succession 
 spread more widely, till, as may now be seen, the uppermost lava-flow forms a wide 
 sheet, covering not only the old rivers and their tributaries, but also most of the 
 lower ridges of Silurian rock which separate them. 
 
 “Throughout all the Newer Voleanic areas are found the points of eruption 
 whence the lava streams issued, mammaloid or conical hills, in many of which well- 
 formed crater-basins still exist, while in others the crateriform shape is_ still 
 distinguishable, though the basin has been obliterated. Many of these extinct craters 
 are now occupied by lakes or lagoons, as Tower Hill, near Warrnambool, which has an 
 insular peak rising from the centre of the lake; Mount Eels, and other crater basins in 
 the western district, and Mount Mercer, south from Buninyong. Mounts Buninyong, 
 Warrenheip, Pisgah, Franklin, and numerous other voleanic hills in the Ballarat, 
 Creswick, Daylesford, and other districts, are familiar instanves of points of eruption 
 where the outlines of the craters are still discernible. 
 
 ‘“‘ Around nearly all such points are scoriaceous lavas and voleanic ashes, among 
 which are frequently found ejected masses of older rocks, from mere dust up to several 
 tons in weight. 
 
 “For instance, in the voleanic ash of the Anakies, near Geelong, are found 
 ejected blocks of granite. At Buninyong and Hardie’s Hill, to the south thereof, are 
 ash beds, composed principally of large and small fragments of slate and schist. In 
 some places, as on the Werribee Plains, near Mount Mary, the ash beds present a 
 stratified appearance, as though their materials had fallen into and had been arranged 
 by water. It is probable that this may have been the case, but there is no evidence of 
 any very considerable submergence since, as, had such taken place, very few, if any, of 
 the volcanic hills, composed as they are of loose incoherent materials, would have 
 preserved their form as we now see them. It is probable, however, as suggested by Mr. 
 Selwyn, that some of them formed low islands in the Tertiary seas.” 
 
 Of the New South Wales Volcanic Rocks, the late Mr. C.S. Wilkinson wrote *:— 
 “ The voleanic rocks, dolerite, basalt, amygdaloid, &c., are almost entirely of Tertiary age. 
 They occur in many places on the high lands of the Great Dividing Range, forming 
 ylateaus, and also upon its eastern and western slopes. They have been chiefly erupted 
 irom ‘pipes or fissures,’ without forming any of those conical hills with crater-basins 
 which so characterise many of the points of eruption in the volcanic districts of Victoria. 
 The lofty Conobolas, near Orange, are, however, extinct volcanoes. 
 
 “In the Gulgong Gold Field we have amygdaloidal basalt containing analcime, 
 stilbite, &c. From its position in regard to the drifts, it is probably of Upper Miocene 
 age; while overlying the Pliocene drifts (deep leads) in the same locality occur extensive 
 flows of basalt, which have filled up old valleys, and here and there spread out over 
 considerable areas. Similar occurrences may be observed in the stanniferous districts 
 of Inverell and in several other parts of the colony. 
 
 ‘ Basaltic rocks occupy some of the highest points of the Dividing Range near 
 Kiandra, as at Mount Table-top, which is over 5,000 feet above the sea, and which the 
 late Mr. Lamont Young, who explored it in 1880, regarded as a point of eruption. 
 
 
 
 
 
 * Notes on the Geology of New South Wales, by C. S, Wilkinson, Government Geologist. Sydney: 
 by Authority : 1882, p. 62, 
 
579 
 
 “Near Inverell the Pliocene basalt contains large crystals of herschelite, with 
 analcime and aragonite, also small rounded masses of olivine. Basalt of the same age 
 caps the Bald Hills, near Bathurst; it here exhibits columnar structure.” 
 
 Referring to the basalts and associated drifts of New England, Mr. T. W. 
 Edgeworth David says * :— 
 
 “During the greater part of that vast period of time (the Mesozoic) the surface 
 of the land was being slowly broken up and worn down by the action of rain, frost, 
 sunshine, vegetation, and perhaps marine erosion, until a land surface was evolved, 
 which in its broad features resembled the present. Vast thicknesses of sedimentary 
 material having been removed by these means, the underlying crystalline rocks were 
 laid bare, and, erosion proceeding still further, the crystalline rocks themselves and 
 their metalliferous veins became disintegrated and their materials transported and 
 redistributed by water. In this way were formed the deposits of gravel, of which the 
 outliers at Scrubby Gully and Ruby Hill are the insignificant remnants. The intensely 
 worn surfaces of the pebbles in this gravel, and the fact that only the hardest and most 
 indestructible minerals—as quartz, tinstone, and gemstones, &e.—have survived in them, 
 shows that they must have been subjected to a long process of battering and bruising, 
 in which the weaker pebbles of claystone, granite, &c., were completely pulverised. 
 The only power in nature capable of doing such a work is the sea, where it breaks on a 
 rocky coast. These Tertiary gravels are, therefore, probably of marine origin, a fact of 
 great significance as bearing upon the probable richness of stream tin of the ‘deep 
 leads,’ for marine beds must have had a wide extent, and the great richness of these 
 small outliers favours the expectation that the far larger portions which have been 
 swept away were equally rich; so that large bodies of ore derived from this source must 
 have gravitated into the lower level gravels subsequently buried under lava. As the 
 land continued to rise the sea would recede further west, and the rivers being increased 
 in size and power subaerial degradation would proceed more rapidly. The channels of 
 the rivers would be continually deepened, and the whole surface of the land gradually 
 lowered to adapt itself to the increasing fall of the rivers. The three terraces of gravel 
 at the Surprise Mines mark the levels at which the bottom of a large river stood at three 
 successive epochs. What was the exact configuration of the country at the time of the 
 first outburst of the basalt lavas geological evidence fails to tell. That part only which 
 has been sealed up under the lava sheets has been preserved to the present day, and its 
 shape is being gradually restored by the workings on the ‘deep leads.’ The results of 
 these subterranean explorations tend to show that most of the country now covered by 
 lava sheets, and forming in places main lines of water parting, was at that time near to 
 or part of the principal drainage channels, and that the trend and fall of these 
 old rivers agreed approximately with that of their nearest modern equivalents. Of 
 course there are no exact modern representatives of these old streams, nor is it always 
 possible to determine, even approximately, with what present rivers they should be 
 correlated. At the Fishing Grounds, however, near Kangaroo Flat, there can be no 
 doubt that the old stream, which produced the coarse shingle now capped by lava, was 
 related to the present Beardy River. The bottom of the channel of the Beardy at the 
 nearest point, one mile distant, is now 550 feet below the level of the bed of this buried 
 river channel. The flora of the period, to judge from the number and variety of leaves 
 entombed in the Hocene pipeclays, was rich and diversified. The fossils are chiefly 
 leaves of herbs, trees, and ferns, some having fruit, and one a blossom delicately 
 
 
 
 
 
 * Geology of the Vegetable Creek Tin-Mining Field, by T. W. Edgeworth David. Mem. Geol, 
 Survey NV. S. Wales, 1887, p. 58. 
 
580 
 
 preserved. At Rose Valley, near Emmaville, the vegetable matter has almost entirely 
 disappeared, the cast only remaining in the white pipeclay, which is stained a rusty 
 yellow where it has received the impressions of the fossils. At Witherden’s tunnel, in 
 portion 50, parish of Hamilton, the fossils are enclosed in a dark brown fine sandy clay, 
 the original material of the leaf being preserved; and at the head of the Wellington 
 Vale Lead, leaves are similarly preserved in a hardened biack silt. A collection of the 
 fossil plants from Rose Valley has been sent to Baron von Ettingshausen, and, as already 
 stated, they are considered by him to contain many types found in the early Tertiary 
 flora of Europe and America; thus establishing the age of the oldest leads near 
 Emmaville as Early Tertiary. Amongst them are several varieties of beech and oak, 
 pines allied to the kauri pine, and Wellingtonian pine, intermixed with banksias, 
 grevilleas, laurels, and eucalyptus. A detailed list and description is given in Baron 
 Ettingshausen’s work now published. Impressions of fossil insects have been found on 
 the Red Hill, near Emmaville, the markings being plainly visible in fine brown earthy 
 ironstone ; but these belong to the later part of the Tertiary voleanic epoch. Ata time, 
 then, when the physical features of the country were somewhat similar to what they are 
 now, and its surface, probably some twenty feet or so higher than at present, was 
 covered with an Eocene flora, voleanie energy revealed itself in the first eruptions of 
 basalt. The hard rocks of the quartz-porphyry, felstone, and granite were rent 
 open; and, where the voleanic forces became centralised, small cones were thrown 
 up composed of comminuted fragments of the underlying rock and_scoriaceous 
 basalt. The lava emanating from these centres poured into the valleys in 
 streams from one hundred to two hundred feet thick, flowing for a distance 
 of from six to twelve miles. Dispossessed of their old beds, the creeks and 
 rivers bad to wear for themselves fresh channels, either down the centre of the 
 lava stream, or along one or both of its margins. It is probable that, in accordance 
 with facts observed in connection with recent lava streams, the sides of these old basalt 
 flows in contact with the cold rim-rocks would cool and consolidate while the centre of 
 the mass was still fluid. The result of this would be that the centre of the stream would 
 flow away from the sides leaving them at a higher level, and so giving rise to a slight 
 central depression. This would favour the erosion of the new channel immediately over 
 the site of the old one, where the lava must necessarily have been thickest and so most 
 fluid, and where consequently the lowest point of the depression should lie theoretically. 
 More frequently, however, the water chose the junction lines of the basalt with the 
 Paleozoic rocks. That the voleanic activity was prolonged for a vast space of time 
 is proved by the extent of denundation which has taken place between the older 
 flows of lava and the newer. The amount of this can be measured at the upper end of 
 - the Vegetable Creek Lead at Rose Valley. The section at Griffith’s and Fox’s shafts 
 shows that a watercourse has cut through one or more flows of basalt altogether 
 to adepth of about sixty feet. Then succeeded another flow of basalt, which buried the 
 second channel to a depth of a hundred feet. These second eruptions appear to have 
 been less violent than the first, the lava welling up, probably from wide rents, and 
 producing the low, gently sloping cones of solid lava, destitute of the volcanic dust and 
 scoria characteristic of the earlier outbursts. Evidence as to which is the latest flow 
 of basalt israther meagre; but judging from the general freshness of the appearance of 
 the lava at Kangaroo Flat, in Portions 70 and 73, Parish of Arvid, it seems to me that 
 this flow is one of the most recent. Powerful streams must have flowed in places over 
 the surface of the basalt long after its consolidation, as evidenced by the coarse Pliocene 
 gravel in Portions 696 and 751, Parish of Strathbogie, where some of the water-worn. 
 blocks are over one foot in diameter. This gravel is, roughly, about one hundred and 
 
581 
 
 fifty feet above the Severn River. At the time such a coarse gravel was formed it is 
 searcely conceivable that the present Severn Valley existed, and its erosion was, there- 
 fore, probably subsequent. Here, however, a question of great difficulty arises. The 
 statement already made, that most of the present river channels have been deepened by 
 from three to six hundred feet since the last lava-flows, is generally correct ; but what 
 appears to be a remarkable exception to the general rule occurs at Strathbogie. Yor 
 about a mile above the head station basalt occurs in position a few feet only above the 
 level of the present river; and, on the left bank of the same river, a shaft sunk through 
 the lava proves that it extends to a considerable depth below the river channel. Alsoon 
 Swamp Oak Creek, one mile north of the north-east corner of Portion 5, Parish of Astley, 
 the basalt comes down within a few feet of the level of the creek. In the latter 
 instance the position of the basalt may be partly due to landslips; but the first case is 
 incapable of such an explanation, and the interpretation of this phenomenon must 
 
 Pe deferred until a geological examination is made of the country south of the Severn 
 iver. 
 
 “These patches of Pliocene river gravel show that at the close of the Tertiary 
 Volcanic period the outpouring of the lava streams by filling up the valleys had locally 
 raised the level of the drainage channels. Running water, however, ceaselessly fretting 
 the rocks, by degrees wore fresh troughs as deep as the old ones, and eventually 
 considerably deeper. The heavy rainfall of the Pleistocene period must have materially 
 accelerated this work of erosion; but in this rocky district, with its steep falls, little 
 trace is preserved of Pleistocene Deposits, except in the wide plains of coarse gravel in 
 the valley of the Dumaresq. The shallow deposits of subangular gravel and sand in the 
 beds of the present creeks and rivers were evidently formed under conditions similar to 
 those which now obtain ; and their stratigraphical position, as well as the occurrence in 
 them of natives’ stone hatchets, proves them to belong to the recent period.” 
 
 From Dalton, near Gunning, there have been obtained the remains of a copious 
 Tertiary land fauna, which Baron von Ettingshausen regards as of Eocene date.* Of 
 this deposit, so far as we know, we have no representative in Queensland. 
 
 In South Australia, as will be seen in the Chapter on the Desert Sandstone, that 
 Formation is sometimes not separable from the Lower Tertiary. It appears as if the 
 emergence of the land which took place in Queensland at or near the close of Mesozoic 
 time did not take place in South Australia till somewhat later. 
 
 We certainly have in Queensland an Older and a Newer Volcanic series, both 
 chiefly basaltic, which may be presumed to be of Tertiary age, although direct evidence 
 of their age is not forthcoming. The absence of evidence on this point may be due to 
 some extent to the fact that the drift deposits beneath the basalts of Queensland have 
 not been explored for gold as they have been in Victoria. 
 
 Our Older Volcanic Series forms extensive beds, which cover the Desert Sand- 
 stone, where the latter is present, or the still older rocks where it is absent. The Newer 
 Series occurs as lava-flows or coulées, which have flowed down the valleys denuded out 
 of the Desert Sandstone or out of the lower basalts. 
 
 OLDER VOLCANIC SERIES. 
 The granitic range dividing the Burdekin and Flinders waters is crossed by the 
 road from Townsville to Hughenden at an elevation of 3,040 feet above the sea-level. 
 The range is flanked on the eastern side by deposits of basaltic lavas extending to 
 
 
 
 
 
 * Contributions to the Tertiary Flora of Australia, by Dr. Constantin, Baron von Ettingshausen. 
 Mem, Geol. Survey N. S. Wales, Pal, i., 1888, p. 9. 
 
582 
 
 Dalrymple, on the Burdekin (see Diagram-Section Pl. 45, fig. 1). On the western 
 side similar basaltic lavas extend to Tatoo Camp, seven miles above Wongalee Station. 
 Here, at an elevation of 1,840 feet, the lowest bed of the basalt is seen resting on the 
 Desert Sandstone. Outliers of the basalt occur between Poreupine Creek and the 
 Flinders as far as Mount Beckford. In all probability it extended over a considerable 
 portion of the Western interior, from which both it and the Desert Sandstone have now 
 been denuded. 
 
 North of Coalbrook Station, on the Northern Railway, fragments of basaltic 
 lava-flows are seen resting on the Desert Sandstone, on the divide between the heads of 
 the Thomson and Flinders Rivers. 
 
 Mr. Rands describes * a basalt about fifty feet in thickness overlying Desert 
 Sandstone in a cafion of the Walker River (Head of the Flinders), which has been cut 
 through both rocks to the depth of two hundred feet. And in the same river, two and 
 a-half or three miles above the junction of the White Mountain Creek, he says,t 
 “The Desert Sandstone is seen faultedagainst the schists by afault running east south-east 
 and dipping south-south-west. ‘The schists and Desert Sandstone are both covered with 
 basalt. The Desert Sandstone is bent up near the fault, and is dipping south-south- 
 west.’’ Here we have an instance showing that a sufficient period elapsed after the 
 deposition of the Desert Sandstone to permit of its upheaval, probably accompanied 
 by faulting and partial denudation, before the basalt was poured over it. 
 
 In the same Report, Mr. Rands describes “a vast table-land of basalt extending 
 for many miles” to the west of the Walker River. ‘ Remnants of this basaltic table- 
 land occur on the east side of the river, between it and Oxley Creek, forming ‘ outliers’ 
 which have been separated by watercourses. The remainder of this basalt has been 
 entirely removed by denudation. The cavities in the basalt are full of zeolites. Thin 
 sections of the basalt under the microscope show it to be made up of a ground mass of 
 small interlaced crystals of felspar, with crystals of olivine throughout it. The olivine 
 crystals are much decomposed, especially around the margins of and along the cracks 
 in the crystals. It contains very little magnetite. The basalt is clearly of Tertiary 
 age, overlying, as it does, the Desert Sandstone.” 
 
 Mr. Rands, speaking of the Cape Gold Field, says :—‘‘ The only instance of basalt 
 on the Cape side of the range is that of Mount Blaek, situated about nine miles west 
 of the Upper Cape. Mount Black is a hill of schist, capped with basalt about two 
 hundred feet in thickness. The latter is a dense olivine-basalt, and has in places 
 assumed a columnar structure. It possesses magnetic polarity.’’t 
 
 An immense area of horizontal basalt occupies the whole district extending from 
 Lake Cargoon and Wandovale on the west to the Burdekin on the east, and from 
 Lolworth Creek on the south to the heads of Emu and Maryvale Creeks on the north. 
 Beds of white pipe-clay are occasionally met with between the beds of basalt. This 
 area is watered by Lolworth, Fletcher's, Allingham’s, Emu, and Maryvale Creeks, and 
 the Basalt River. In Maryvale Creek the ‘‘ Diprotodon-breccia” described by Daintree 
 occurs, so that we here have the age of the basalts defined so far as that they lie 
 between the Upper Cretaceous and the Post-Tertiary. The basalts of this area are 
 known to overlie, at least in their northern portion, gold-bearing drifts, which, however, 
 have never been prospected to any extent. . 
 
 Further north, between the heads of the Broken River (a tributary of the 
 Clarke) and those of the Hinasleigh, horizontal beds of basalt cover a wide stretch of 
 
 * Report on the Cape Gold Field. Brisbane: by Authority ; 1891, p. 11. 
 t+ Loc. cit. 
 ~ Ann, Progress Report Geol. Survey of Queensland for 1890, Brisbane: by Authority : 1891. 
 
583 
 
 country, resting apparently on the eastern side on the “ Star Beds,” and on the western 
 on mica schists and granites. This area is thus described by Mr. Maitland in his 
 Report on the “ Geology and Mineral Resources of the Upper Burdekin ”’* :-— 
 
 “The basaltic lavas oceupy an area of about two thousand square miles at the 
 head of the Burdekin. 
 
 “The largest development occurs in the corner near the divides between the 
 waters of the Burdekin and the Hinasleigh, and between the Herbert and the Burdekin ; 
 they form an extensive plateau, having an average altitude of about two thousand 
 feet above sea-level. The western boundary of this immense plateau has not yet been 
 mapped. 
 
 ‘“Basaltic outflows are known to exist at Surprise Creek, a tributary of the 
 Einasleigh. These, which emanated from foci, on the Burdekin-Einasleigh Plateau, are 
 erossed by the coach road from Herberton to Georgetown, near Quartz Hill. This is 
 distant about forty miles from the watershed of the Burdekin and the EHinasleigh. 
 
 “The northern boundary has also not been delineated. Streams of lava have 
 flowed down some of the existing valleys in the neighbourhood of Gunnawarra Station, 
 and have been described in a previous report.t Doubtless the hot springs therein 
 described is but the ‘dying gasp’ of that volcanic action which was at one time rife 
 in this district. 
 
 “Tn addition to this immense plateau, there occur other isolated patches in.the 
 district, shown on the map. These lavas, since their formation, do not appear to have 
 been very much affected by denudation. 
 
 “The basalt, of which the tableland is made up, occurs in a series of super- 
 imposed lava-flows, emanating from numerous voleanic foci, which rise as conspicuous 
 hills all over the plateau. 
 
 “The surface of these lavas is, in places, formed of ‘chaotic heaps of angular 
 blocks of basalt, tossed in every variety of disorder,’ rendering locomotion a matter of 
 some considerable difficulty, especially with horses. Generally, the surface produces a 
 luxuriant growth of vegetation, well suited for and much relished by stock. The more 
 tugged surfaces of some of the more recent flows are covered with bottle-tree scrub. 
 
 “On the other side of the Burdekin, west from the Valley of Lagoons Station, 
 the surface of the lava-flows is full of dismal-looking deep pits, of all dimensions, in 
 which water often accumulates. The formation of these pits appears to be due to the 
 caving in of the surface of a lava stream. The surface of a lava stream flowing from 
 one of the volcanic foci cools and hardens, whilst the molten matter flows from beneath, 
 leaving a tubular cavern; in course of time, a portion of the hardened surface gives 
 way, and a pit with vertical sides is the result. These caverns can sometimes be followed 
 for a considerable distance ; they form excellent hiding-places for the natives. Water 
 can often be seen and heard flowing at the bottom of these holes. Many of these large 
 holes, filled with water, are met with on the divide between the Herbert and the 
 Burdekin. In the whole of the area examined there was found no trace of any 
 fragmental rocks associated with the basaltic outflows. It is conceivable that denudation 
 may have removed all trace of the more incoherent material ejected ; but still it is hardly 
 likely that in an area of twothousand square miles there would not be some fragments left 
 
 “ Professor J. D. Dana,t in the course of his studies in vuleanology, has concluded 
 that basaltic lavas are but rarely associated with fragmental deposits (ashes, cinders, and 
 
 * Brisbane: by Authority: 1891. 
 
 + “The Geology of the Coolgarra Tin Mines and Surrounding Districts.” A, Gibb Maitland. 
 Brisbane : by Authority; 1891. 
 
 + J. D. Dana, Characteristics of Volcanoes, London: 1890, 
 
584 
 the like). When such discharges do take place, they are usually occasioned by the 
 diminution of the internal heat. Hence it would appear that ashy deposits from basaltic 
 volcanoes are among the last stages in their history. 
 
 “In the Cooktown and the Herberton districts there do occur beds of ashes 
 which emanate from basaltic cones; but whether these are of later date than the 
 Burdekin-Hinasleigh lavas, yet awaits proof. 
 
 “Throughout the area occupied by the lavas, there is a very great difference both 
 in texture and colour. Some portions are very vesicular and slaggy, whilst others have 
 that peculiar ‘ropy’ or wrinkled appearance, characteristic of lava streams, which have 
 flowed slowly from their source; others, again, are fairly compact. In colour they 
 vary from bluish-grey to bright red, with all degrees of variation. In cavities in the 
 basalts beautiful specimens of chalcedony can sometimes be seen. 
 
 “The black soil formed by the decay of the rocks is often crowded with fragments 
 of semi-opal. 
 
 ‘“A number of slices of the basalts have been prepared and submitted to 
 microscopic examination. 
 
 “A partial analysis of a specimen from the Valley of Lagoons has been made for 
 me by Messrs. Coane and Clarke, Charters Towers, with the following result :— 
 
 Combined silica ... ves ae aise sa¢ wea ... 43°8 per cent. 
 Free silica... va rhs tS oe as = Os » 
 Tron Nas ‘ A i ASG » 
 
 “One example—viz., that from Mount Razorback—would be more correctly 
 described as a magma-basalt, from the fact that the minerals are scattered through a 
 glassy matrix or magma, which by ordinary transmitted light is of a brownish colour. 
 This, however, is merely a local occurrence; afew yards distant from the summit of 
 Mount Razorback the basalt resumes its ordinary type. 
 
 “The felspars, which make up the larger portion, occur as long lath-shaped 
 erystals, showing plagioclastie twinning. They are remarkably clear and fresh, and 
 contain numerous minute inclusions. 
 
 “Olivine, in erystals and crystalline grains, is altered along its edges into a 
 ferruginous product. Sometimes the whole of the crystals and grains have undergone 
 this alteration, but generally the decomposition is found to extend only a short distance 
 from the periphery. 
 
 “The augite occurs in long brownish crystals, often showing faint dictoroism, 
 and magnetite in grains, 
 
 “Tn the slices of any of the basalts which were examined, there occurred a little 
 clear transparent isotropic matter. 
 
 “Some portions of the glassy matter contain minute particles of some doubly 
 refracting mineral (quartz ?). 
 
 “The partial analysis made by Messrs. Coane and Clarke shows the presence of 
 a sinall quantity of free silica, and to this the isotropic matter may be referred. 
 
 ‘There existed no primary quartz in any of the slices of these basalts. 
 
 “All over the plateau numerous small ‘ puys,’ the remains of orifices from . 
 which these basaltic lavas emanate, are met with. 
 
 “ Ascending the Valley of Reedy Brook to its head, and crossing the divide into 
 the waters of Gunnawarra Creek, a tributary of the Herbert River, a good idea of 
 the mode of occurrence of the lavas and the structure of the volcanic foct can be 
 obtained. ; 
 
 “Much more work will be necessary before a full description of the whole of the 
 sources of the lava on the plateau can be obtained. 
 
585 
 
 “Mount Lang is situated on the eastern bank of one of the heads of Kinrara 
 Creek; its summit is about four hundred and forty feet above its base. The hill 
 presents a steep face to the west, with a somewhat gradual slope to the east, and is 
 formed of very vesicular basalt, which sometimes has a reddish hue. Its western face 
 has a vertical wall of bare basalt, through which fragments of scoria are scattered. 
 Round about the base the fragments of basalt have a tendency to weather into rudely 
 hexagonal blocks. 
 
 “Teaving Mount Lang and travelling almost due north, with the object of 
 reaching Mount Razorback, several minor ‘ puys’ are passed. . These were only visible 
 when in close proximity, owing to the dense timber. 
 
 “ About three miles from Mount Razorback, and to the south-west of it, a 
 conspicuous hill formed of vesicular basalt was examined. This hill is in shape semi- 
 circular, with its diameter running north-west and south-east. It is a breached lava 
 cone, the stream flowing north-east from it and thence down one of the heads of 
 Anthill Creek. 
 
 “Mount Razorback is situated in the northern portion of the area, and is by 
 far the largest and most conspicuous of any of those occurring within the Burdekin 
 watershed. 
 
 “Its shape is that of a long razor-backed ridge, with a conspicuous eminence 
 forming its highest summit, which, by aneroid, is 680 feet above its base. The 
 mountain is composed of basalt of a reddish colour near its highest point, but of a 
 bluish-gray throughout. 
 
 “ The basalt is very vesicular and somewhat glassy in places. From the summit, 
 as many as twenty-five minor ‘ puys’ are visible; these appear to be much more 
 plentiful to the west. They assume all shapes and sizes; sometimes merely a slight 
 elevation marks their position, as though the molten matter had merely oozed out from 
 an orifice and flowed away on all sides. 
 
 “ Tn other parts of the district outlying patches of basaltic lavas are met with. 
 
 “‘ A well-marked area is to be seen in the vicinity of Mount Fox, near the head 
 of one of the tributaries of the Douglas River. 
 
 “ Mount Fox, an extinct volcano, is the culminating point of this area. Its 
 altitude is 2,870 feet above sea-level. In shape it is a truncated cone. The summit 
 comprises an area of two or three acres, surrounded by a low semicircular wall, about 
 thirteen to fourteen feet in height, on the north, with a shallow hollow or depression in 
 the centre. To the south this wall has been breached by a lava which flowed down that 
 side of the mountain, filling up all the inequalities of the surface, and forming a plain 
 of no inconsiderable extent. 
 
 “The mountain is almost devoid of timber, save a few patches of scrub on four 
 sides. The portions devoid of timber are covered with sheets of vesicular lava, now 
 broken up into blocks of all shapes and sizes. These timberless portions, now overgrown 
 with long grass reaching to a height of about 2 feet, mark the site of old lava flows. 
 
 “ From the western side of the peak a conspicuous flow follows the eastern bank 
 of a gully flowing south-west at a considerable elevation above the creek. The flow 
 ends abruptly to the south-west; its surface is covered with blocks of compact basalt. 
 
 “ All round the mountain denuded tables of basalt can be seen. A conspicuous 
 one consists of a semicireular ridge of compact lava, about 30 yards in width, trending 
 generally north-west for about a quarter of a mile. The summit of this is about 2,310 
 feet above the level of the sea. 
 
 “ Nearly due west from this a section, at an altitude of 2,220 feet above sea-level, 
 shows the basaltic lavas resting on a bed of quartzose grit. 
 
586 
 
 “‘ The hill, 2,475 feet high, to the south-west of the section, is formed of a series 
 of successive sheets of lava. 
 
 “Tt is impossible to estimate the thickness of the basalt on the plateau, because 
 there are no data available which will enable an idea to be formed as to what was the 
 form of the ground before the lavas were poured out ; and, further, there is no record 
 of their ever having been penetrated by any excavation. 
 
 “The age of these basaltic outflows has not yet been definitely fixed. The lavas 
 rest in turn upon all the other rocks in the district; one section, seen near the Valley of 
 Lagoons Station, shows them resting directly upon the Desert Sandstone Beds. The 
 basalts, therefore, are younger than the Upper Cretaceous. 
 
 “Mr. Daintree conjectured (presumably on account of their lithological 
 similarity) that the lavas to the ‘north of latitude 21° were probably the equivalents 
 of the “Upper Volcanic series’”’’ of Victoria which were referred to Pliocene- 
 Tertiary.* 
 
 “ Lithological similarity is not to be safely relied upon in determining geological 
 age; still there is strong presumptive evidence that all these basalts have been emitted 
 at approximately the same time. 
 
 “These Upper Burdekin lavas are in all probability Tertiary, but as to the 
 exact horizon to which they are to be assigned no evidence has yet been collected.” 
 
 It is impossible, on reading the above account, to avoid suspecting that in the 
 above notes Mr. Maitland is describing basaltic outflows of different ages—an older, to 
 which the bulk of the basaltic tableland belongs, and a newer, to which may be referred 
 the ‘‘puys” or foci still remaining in a remarkable state of preservation, and in all 
 probability the flows of basalt which come down the valleys below the edge of the 
 basaltic tableland. One of these comes down the Valley of Reedy Brook, washed on 
 either side by its tributaries Kinrara and Reedy Creeks. This flowis at least twenty-five 
 miles in length, and I was informed by the late Mr. Scott, of the Valley of Lagoons, 
 that it emanated from a crateriform hill near the head of Kinrara Creek. 
 
 Beds of white pipeclay are occasionally met with between the beds of basalt on 
 the tableland. 
 
 On both sides of the range which divides the upper portion of the Herbert River 
 on the west from the Johnstone and Barron Rivers on the east, are large plateaux of 
 horizontally-bedded basaltic rocks. On the western side the thermal spring of Innot’s 
 Creek remains to attest that the volcanic activity has not yet entirely died out. Mr. 
 Maitland has furnished the following Notes on a specimen of the basalt from this 
 nly after a microscopical examination :— 
 
 “Specimens collected from the bed of Prior Creek—one of the heads of Mazzlin 
 Creek, a tributary of the Barron, at the crossing of the Port Douglas and Herberton 
 road, where beds of coarse vesicular basalt alternate with others of much finer grain— 
 were found to be of bluish-gray colour, with small grains of olivine set in a fine-grained 
 matrix. Examined under the microscope the rock is found to consist of a fine-grained 
 matrix, made up of lath-shaped plagioclase felspar, augite, and magnetite, through which 
 large crystalline grains of olivine are scattered. 
 
 “The felspars, which form by far the largest portion of the rock, are remarkably 
 clear and fresh. Under a high power they are seen to contain glass-inclusions, minute 
 needles of apatite (?) and colourless microliths of augite. 
 
 “The ferro-magnesian constituent, augite, never occurs porphyritically, but 
 always as a constituent of the ground-mass. Well-defined crystals are absent, the 
 
 
 
 * Quart. Journ. Geol. Soc., xxviii., p. 318, 
 
587 
 
 usual form being irregularly shaped granules and granular aggregates, devoid of 
 cleavage. One of the minute colourless augites, presenting the usual eight-sided 
 outline, shows what are undoubtedly lines of accretion. 
 
 “The crystals of olivine present all the characters common to olivines of basaltic 
 rocks. 
 
 “Trregularly shaped grains of magnetite are of common occurrence. 
 
 “A little clear, glassy matrix can be detected.” 
 
 On the eastern side of the range, the basalts, in horizontal beds, form a tableland 
 at an elevation of between 2,000 and 3,000 feet, extending from the brow of the Coast 
 Range to the base of the Herberton mountains. The tableland is covered with a most 
 magnificent tropical jungle, through which hardly a ray of sunshine can penetrate. The 
 basaltic soil and a heavy rainfall have combined to produce in this region an almost 
 incalculable wealth of cedar and other valuable timber. 
 
 Accompanied by Mr. Maitland, I visited, in 1889, the “crater-lake,’’ Lake 
 Eacham. The lake occupies the very summit of the divide between the heads of 
 Petersen’s Creek (Barron Waters) and the heads of creeks flowing into the Mulgrave. 
 It is located, but not named, on the Two-mile Map issued by the Department of Lands ; 
 but is minutely charted in the “ Plan of the Village of Eacham, Parish of East Barron,” 
 issued by the same Department in 1889. I observe that Mr. A. Meston* spells the 
 name Yeetcham, as more in accordance with the native pronunciation. Mr. Meston 
 briefly describes another lake, named “ Boonoobagolomee,” seven or eight miles to the 
 west, and adds :—“ The blacks speak of a third lake much smaller than the others, but 
 so far [October, 1889] it has not been seen by white men.” 
 
 My companion and I reached Lake Eacham by a track from Halfpap’s Hotel, in 
 “ Petersen’s Pocket,” on the Cairns and Herberton pack-road. At the junction of the 
 roads from the Mulgrave and Russell Gold Fields to Cairns, we found a tree marked 
 “ Lake 400 yds., 8.W., J. MeL., R. Hood.” From this point we made a considerable 
 ascent to the highest point of the ridge surrounding the lake, where we found a tree 
 marked 84 over V., which we understood to be the south-east corner of an “ Agricultural 
 Area,” and another marked with the name of the discoverer and the date of discovery, 
 “J. McLellan, June, ’79.” This point, from which the first glimpse of the lake was 
 obtained, was 2,680 feet above sea-level by Aneroid measurement. The descent to the 
 lake was very steep, and, like all the rest of the day’s journey, clothed with dense jungle. 
 The Aneroid gave the surface of the water as 2,390 feet. 
 
 The lake is surrounded by a ridge composed of loose weathered volcanic ash, 
 containing stones up to six inches in diameter, mostly of bombs of a doleritic reck full 
 of olivine. In ascending the lip of the lake we came on rocks in sifu which we had 
 missed in the descent. These were of rudely stratified “ash’’ of angular fragments, 
 dipping at 5° away from the lake. The lake has neither affluent nor effluent; and 
 as it stands higher than the surrounding country, and is enclosed by a wall of ashy 
 materials heaped up above the level of the basaltic tableland, I think it is very probable 
 that it really occupies a crater. It is clearly impossible that, in the latitude where it 
 occurs, the lake could have been hollowed out by an ice-sheet, which would, moreover, 
 have levelled the surrounding rim of soft ash. The lip of the crater is not of uniform 
 height ; and although it is likely enough that it has suffered greater denudation in some 
 places than in others, it may be conjectured that the greater height of the rim on the 
 western side may be due to some extent to the tendency of the prevailing south-east 
 winds to drive the ejected materials to the leeward. The lake is said to be of vast depth, 
 
 * Report on the Government Scientific Expedition to the Bellenden-Ker Range. Brisbane: by 
 Authority : 1889. 
 
588 
 
 and to contain no fish. At any rate, we saw none. Neither did we see any water-fowl, 
 which are said also never to visit the lake. There was nothing in the taste of the water 
 to account for this absence of life, if it be a fact. The highest flood-marks we saw were 
 about three feet above the water. It must be remembered that we visited the lake at 
 the latter end of an unusually protracted drought. The slight variation of level might 
 be accounted for by the fall of rain on the lake and its banks on the one hand, balanced 
 by evaporation and leakage on the other. 
 
 The ‘Volcanic Hill’”* marked on the map in “ Pinnacle Pocket,” on the right bank 
 of the Barron, between the mouths of Leslie and Petersen’s Creeks, stands about 200 feet 
 above the level of the basaltic tableland, and is composed of a highly scoriaceous basalt 
 very rich in olivine. There are said to be several similar hills in the jungle in the neigh- 
 bourhood, and in all probability they are “necks” or ‘ plugs’’—7.e., volcanic orifices 
 filled up with solidified basaltic lava. 
 
 It is interesting to find two volcanic craters almost side by side, the one filled up 
 with hard lava-form rock, and the other surrounded by friable ejected ash and forming 
 a crater-lake. It is just possible that in spite of their proximity they may be of different 
 ages, the “ plug” belonging to the ‘‘ Older”? and the ‘‘crater-lake ’’ to the “ Newer” 
 Volcanic series. Or they may even both belong to the latter. 
 
 On the Russell River, south of Mount Bartle Frere, gold is obtained in considerable 
 quantities, mixed with stream tin ore and (rare) platinum, from gravelly drifts which 
 rest on slates and schists, and are overlaid by horizontal beds of basalt. The basalt is 
 one of many denuded fragments which once formed a part of the immense plateau 
 extending southward from the Mulgrave to the heads of the North Johnstone and west- 
 ward to nearflerberton. In Messrs. Clarke and Joss’s Claim, which is the south-eastmost 
 working, the edge of the basalt is seen to overlie a siliceous sandy silt permeated with 
 iron peroxide. The silt shows alternate layers of coarser and finer material, and is in 
 places cross-bedded. It rests on a “ washdirt” mainly composed of well-rounded quartz 
 boulders. There are no basalt stones in the wash, and no boulders of granite. 
 The latter circumstance is hard to account for in a valley where granite is 
 frequently to be met with zz situ. The washdirt varies in this claim from 2 inches to 
 30 inches in thickness. Between the washdirt and the slaty bed-rock avery fine white 
 siliceous silt, a few inches in thickness, generally intervenes. The fact that this silt is 
 traversed by a few thin veins of quartz renders it probable that the sand was formerly 
 cemented into a sandstone, but has lost its cement after the formation of the quartz 
 veins. 
 
 The outcrop of the washdirt has been opened out along the south-eastern and 
 north-eastern side, and a tunnel has been driven through the washdirt for 135 feet from 
 S. 10° E. to N. 10° W. This tunnel is connected with another running 50 feet 
 to the east. Another tunnel has been driven 70 feet to W. 10° S. from a 
 point on the hillside 120 feet N.W. of the northern end of the long tunnel. At the 
 inner end of the 70-feet tunnel the slate bottom rises up and the basalt comes into direct 
 contact with it. This tunnel is only used as a reservoir, from which the water is 
 conducted to the tip at the end of a tramway leading from the mouth of the long tunnel. 
 The basalt is in some places at least forty feet thick, but is often decomposed throughout 
 its entire thickness. It rests, as seen in some places (of which there is an example in 
 an opening near the south corner of the claim), directly on the washdirt, the absence of 
 the upper silt proving that it was poured out over an uneven and denuded bottom. 
 
 * “Volcanic” is scarcely distinctive enough in the midst of a volcanic region, but the “hill” in the 
 midst of the basaltic plateau is a conspicuous feature, 
 
589 
 
 The washdirt from the long tunnel gives prospects equal to about half-an-ounce to the 
 load, the gold being in very fine grains. Minute flakes of platinum are occasionally 
 found among the gold. 
 
 In Burns and Party’s workings (half-a-mile to the north-west of Clarke and 
 Joss’s), a red decomposing basalt rests on yellow sand which overlies ten or twelve feet of 
 gravel in coarser and finer layers. The gravelly washdirt is irregularly cemented by 
 brown hematite. It has gold throughout, which, however, can only be saved from the 
 unconsolidated portions. The bottom is of slate with numerous quartz veins. 
 
 In Butler and McDonald’s Claim, a quarter of mile north of Burns and Party’s, 
 a drive has been made under the basalt. On a bottom of decomposed slate and grit is 
 a cemented gravel about one foot in thickness. On this lies a gravelly wash, having a 
 thickness of two feet and under. The washdirt occasionally has fifteen feet of soft 
 white sand above, and occasionally a few inches of fine siliceous silt beneath, as in 
 Messrs. Clarke and Joss’s claim. A shaft above -the workings passed through ten feet 
 of basalt, fifteen feet of sand, and five to six feet of gravelly wash. I saw some good 
 prospects washed from the dirt. Slates and greywackes are seen in the gulley, striking 
 to W.N.W. 
 
 In Robinson and Anderson’s Claim, a quarter of a mile further north, a drive 
 shows a very bouldery gravel from two and a-half feet in thickness and under, lying 
 between the slate bottom anda fine white sand. The bottom is very uneven. In one 
 place there is no sand or gravel between the basalt and slate. An open cutting south 
 of the drive showed a fine white sand lying on from eighteen inches to two feet of fine 
 gravelly wash with lumps of ferruginous cement at its base. The bottom was slate. 
 The upper part of the gravel gave 2 dwts. gold per load, and the lower part none. It 
 may be mentioned that Robinson was nearly killed (on 4th January, 1888) by a native 
 who attacked him with a tomahawk while he was engaged in laying down a rail. 
 
 Sampson’s Claim is on an isolated hill about a hundred feet below the level of the 
 others, and about half-a-mile east of Robinson and Anderson’s. A shaft has been sunk 
 through sixty feet of basalt and four feet of gravelly washdirt, and a tunnel had been driven 
 from N.N.W. for 150 feet towards this shaft from the outcrop of the wash. The slate 
 bottom is seen at the mouth of the tunnel. About fifty feet in there are two and a-half 
 feet of gravelly washdirt capped by basalt and resting on a slate bottom. Attbis point 
 the tunnel had caved in. A little sand was seen on the gravel a few feet short of the 
 cave-in. I saw some very good prospects washed from the dirt taken from the shaft. 
 
 The gold in the wash of the Terraces is always so fine that it is difficult to prevent 
 some of it floating out of the prospecting dish. A few ounces of fine-grained stream tin 
 always remain in the bottom of the dish, and the separation of this from the gold is a 
 very tedious process—indeed, with the most careful manipulation a proportion of the 
 gold is always left in the residue of tin ore. 
 
 Even at the edges of the drift from which the basalt has been denuded, washing 
 by hydraulic pressure is impracticabie, as the trees of the jungle would fall and obstruct 
 the faces. Buta convenient and unfailing supply of running water is always at hand 
 for sluicing the gravel, which can be shot down to the sluice-boxes. 
 
 The average yield from washdirt reported in Victoria for 1883 was 1 dwt. 20°32 
 grs. ; for 1884, 3 dwts.; and for 1885, 1 dwt. 10°59 ers., per ton. I am certain that the 
 terraces of the Russell River will give a much higher yield than this. The limited 
 workings now opened up are likely to prove only the beginning of an industry which for 
 many years to come will employ the energies of thousands of workmen. The basalt left 
 on the top of the ridge between Cooppooroo and Wairambar Creeks is a narrow tongue, 
 on both sides of which the auriferous drifts which it has preserved from denudation are 
 
590 
 
 easily accessible. But an immense area of the basalt stretches from the Mulgrave to the 
 heads of the Johnstone and westwards to near Herberton, and under this the auriferous 
 drifts probably remain intact. | 
 
 It seems probable that the Valleys of the Mulgrave, Russell, and Johnstone 
 were dammed up by a voleanic outbreak, so as to form a vast lake, in which for a time 
 a fine siliceous sand was quietly deposited ; that the barrier was at length broken down 
 by the stream at the outlet of the lake, and numerous torrents:removed the greater 
 part of the sand and brought down gravel charged with gold; that a second barrier 
 was thrown up and a great thickness of fine silt again deposited ; and that over the 
 nearly level surface thus produced immense flows of basalt were finally poured out, 
 filling up the lake. The waters draining this area, if the lake had not been filled up, 
 would have found their way to the sea by a single outlet, instead of forming as they do 
 three independent rivers. ‘The immense amount of denudation since the outpouring of 
 the basalt is evident when we consider the number and depth of the valleys, which have 
 been carved out, in places, to adepth of more than a thousand feet, through basalts, older 
 river and lake beds, and slate and granite rocks; but the lesson will be impressed more 
 deeply than any description could do on anyone who ean stand on a neighbouring 
 eminence and try to reconstruct, in his mind’s eye, the shores which contained the lake.* 
 
 Gold has for some time been worked, chiefly by Chinese, in the Recent alluvia 
 of the Russell and Johnstone. This gold, which is mixed with stream tin, in all 
 probability came, for the most part, from the “leads’’ under the now denuded basalt. 
 Probably only a small portion of the alluvial gold came directly from the reefs exposed 
 in the slate and granite country since the denudation of the basalt, as a comparatively 
 small area of this country is yet exposed, and not many reefs are known in it. 
 
 I am informed by Mr. John Falconer that on the dividing range between the 
 Dawson and Condamine, lava-form beds of basalt overlie the Desert Sandstone in 
 places. - 
 
 I have also been informed that a cake of basalt overlies the fragment of the 
 Desert “andstone left on the crown of the ridge dividing the head waters of the Langlo 
 River from those of the Coorni Paroo, between Tambo and Adavale. 
 
 It may be thought remarkable that numerous sheets of lava should have been 
 poured out, one after another, and retain such an even surface. No doubt the fact that 
 this has been the case argues a high degree of fluidity in the lava. Some remarks by 
 Captain Clarence E. Dutton, of the United States Army,t on the Volcanic Rocks of 
 the Zuni Plateau, New Mexico, may be quoted on this point :— 
 
 “Jt is plain that the lava sheet which forms the capping of the mesa was 
 gradually accumulated by the repeated outpourings of numberless local vents thickly 
 scattered over its broad surface. And yet it may seem a little strange at first that this 
 diffuse form of volcanic action should have produced a surface which is so little 
 diversified. Judging by the analogy of other regions we should have expected to find 
 the thickness of the lava-cap extremely irregular and studded with large cones with 
 intervening valleys of considerable depth. In reality the thickness, as we recede from 
 the base of Mount Taylor, diminishes very slowly, and even at the extreme northern 
 end is quite three hundred feet. In truth Mount Taylor does not appear to have con- 
 tributed much, if any, to the lava which is more than five or six miles from the 
 immediate base of its cone. The surface of the mesa away from the mountain is but 
 little diversified, and the local cones are for the most part insignificant features. All 
 
 
 
 
 
 
 
 * Report by R.L.J. on the Geology of the Russell River. Brisbane: by Authority : 1888. 
 + ‘Mount Taylor and the Zufii Plateau” in Sixth Ann. Report U. S. Geol. Survey, 1884-85. 
 
591 
 
 this indicates a rather mild type of voleanic energy, in which the eruptions were not 
 highly explosive but only moderately so. The more violent eruptions are attended with 
 the ejection of great quantities of fragmental products, while the milder ones disgorge 
 little else than flowing lava. It is well known that the greater the amount of frag- 
 mental ejecta, the steeper and more compact is the cone or mountain built up around 
 the vent, while the fluent lava spreads out over wide areas, often flowing great distances, 
 - and the slopes which it generates are much gentler and sometimes imperceptible to the 
 unaided eye. As already remarked, fragmental ejecta are common here, and I have seen 
 none at all away from Mount Taylor except the lapiili in the cinder.cones. We shall 
 appreciate this mode of growth of a great lava-cap when we come to study the modern 
 lavas in the San José Valley, where their freshness enables us to see every detail of the 
 process. 
 
 “We may infer, then, that the state of affairs in the region now occupied by the 
 valley of the Puerco was, during the activity of the vents now represented by the necks, 
 much the same as that which is indicated in the mesa above. From 1,000 to L,500 
 feet (according to locality) of Cretaceous strata, since eroded, then overspread the 
 valley and regions to the eastward and southward, also to the northward, from which 
 they have been swept away. Over their surfaces the lavas were outpoured from many 
 vents. The eruptions were of a ‘mild’ type, attended with little violence, and the ejecta 
 were doubtless lava with few fragmental products. These streams, issuing from many 
 vents, became interwoven with one another, and through a long period of time accumu- 
 lated, sheet upon sheet, to great thickness, just as they have done in the valley of the 
 San José in modern times. The result was a lava-cap differing in no respect from that 
 which is now seen upon the surviving mesas.” 
 
 NEWER VOLCANIC SERIES. 
 
 The grounds on which I separate the Post-Mesozoic Volcanic rocks into a Lower 
 and Upper Series are ,(1) that the former was laid down after the elevation of the 
 Desert Sandstone, but before it had suffered any considerable amount of denudation, 
 while the latter was laid down after the former had suffered denudation, in some cases 
 sufficient to allow of the Desert Sandstone and even of underlying formations being 
 exposed ; and (2) that since the deposition of the former, most, if not all, of the vents 
 from which the lava was poured out have been removed by denudation, while the vents 
 of the latter series are still extant, either as crateriform hollows, crater-lakes, or 
 “necks,” filled with plugs of basalt or ash. 
 
 To the latter (the Upper) Series belong the basaltic rocks north of Cooktown 
 Basalt has emanated for the most part from voleanie centres, which occur generally in 
 the form of dome-shaped unwooded eminences near the heads of the valleys which have 
 been denuded out of the sandstone tablelands. Conspicuous among these are the 
 Sisters,” at the head of the Endeavour, the “ Piebald Mountain,” Mount Morgan 
 (Cooktown), &c. These hills do not present a crateriform appearance, but are mere 
 rises, marking the site of the lava eruption, which has spread around them when situated 
 on level ground, or escaped in glacier-like cow/ées down the valleys. These points of 
 eruption bear, in fact, such relation to the lava-flows as the similar foci in Auvergne 
 bear to the basalt there. Coulées of basaltic lava have flowed, from the foc above 
 referred to, down the Valleys of the North and South Forks of the Endeavour River, and 
 have radiated out from Mount Morgan and other centres to the east and north, over the 
 flats between the mountains and the sea, where they form by their decomposition a 
 - chocolate-coloured soil of great depth, peculiarly fitted for agriculture, 
 
592 
 
 Where the basalt bas decomposed into soil on the spot it gives rise to open, 
 well-grassed country, almost bare of trees. Where, on the other hand, the soil has been 
 re-deposited in alluvial flats on the sides of the river courses, it is usually covered by 
 dense tropical jungle. 
 
 The surface of the basalt couwlées, as well as of the dome-shaped centres of 
 eruption, are frequently scoriaceous in a marked degree, forming spongy masses, light 
 and porous as pumice-stone. Occasionally the basalt of the coulées is columnar, as at 
 the Waterfalls in the Endeavour, between Williams’s Station and Brannigan’s. There 
 the basalt is of the usual character, but contains occasional hornblende crystals and 
 much olivine. It also contains lievrite in geodes. 
 
 Gate’s Look-out isa volcanic centre of a different character—the once deep-seated 
 stump or “neck” of a crater, which discharged showers of ashes from its mouth. It 
 forms a conspicuous mountain of tuff, and can be seen from Isabella Creek to cut 
 through the escarpment of a thick bed of the Desert Sandstone. Therock is anagglomerate 
 of volcanic débris, with a certain rude bedding—courses of larger alternating with 
 courses of smaller bombs—having a dip to the east at about 15°. That the 
 bombs are not detached fragments of an already consolidated rock, but have been 
 consolidated from a molten mass while whirling through the air, is proved by the 
 spherical envelope of vesicular basalt which invariably enfolds them. The interior of 
 the bombs, which range from an eigbth of an inch to a foot in diameter, is a mass of 
 black and green crystals of augite and olivine.* 
 
 The Morgan Tableland is a fragment of the Desert Sandstone, about four miles 
 across, and resting on upturned slates. Near its northern extremity a bald—z.e., 
 treeless—mamelon, another of the voleani foci, rises out of the slates, below the level 
 of the Desert Sandstone. Another, which I was unable to visit owing to the prevalence 
 of “ Devil-Devil” country of a very pronounced type, was seen about three miles east 
 of the Morgan Tableland. ei 
 
 Below the level of the tableland of Older Volcanic rocks, a flow of basaltic lava 
 partly fills up the Valley of the Mulgrave River, and doubtless covers alluvial deposits. 
 This lava must, of course, have been poured out after the Older Volcanic rocks 
 abutting against the granitic Bellenden-Ker Range had been cut through by the 
 Mulgrave. 
 
 In the Herberton Deep Lead, stream tin ore in considerable quantities has been 
 obtained from a gravelly wash beneath a capping of basalt, which fills up the Valleys of 
 Nigger Creek and the Wild River. The wash rests on granite. 
 
 Some remarks on the basalt-flows down the Valley of Reedy Brook, &c., and 
 volcanic foci, which I suspect belong to the Newer Voleanic period, although occurring 
 in connection with Older Volcanic lavas, will be found on page 584. 
 
 In the neighbourhood of Gunnawarra Station (Herbert River waters) “ the 
 prevailing rocks are vertical schists overlain in places by sheets of basalt, which appear 
 to occupy portions of some of the existing valleys.” + 
 
 Besides the localities above referred to, basaltic lavas occur in the following 
 places under conditions which show that the Desert Sandstone had been denuded before 
 they were poured out :— 
 
 California Creck (Tate River).—The floor of the valley above the tin-mining 
 township of Ord is covered by a flow of doleritic lava. 
 
 
 
 * Report by R.L.J. on Explorations in Cape York Peninsula, 1878-9. Brisbane: by Authority : 
 1881. : 
 
 + Report on the Coolgarra Tin Mines and Surrounding District. By A. Gibb Maitland. Brisbane: 
 by Authority: 1891. 
 
593 
 
 Lynd River.—A coulée of basaltic lava has flowed down the Valley of the Lynd. 
 The coulée is two miles in width where it is crossed by the Herberton and Georgetown Road, 
 covering the whole of the district between the Lynd and Fossil Brook. Fossil Brook is 
 remarkable as being a strong running stream even in seasons when the Tate, the Lynd, 
 and other larger streams in the neighbourhood are dried up. The permanence of streams in 
 basaltic country has often been remarked. The basalt of Fossil Brook rests on gneiss rock. 
 
 Black Springs.—On the same road, further west, a basaltic cowlée, about a mile 
 in width, occupies the valley of the creek which takes its rise at the Black Creek. 
 
 Surprise Creek.—In the bed of Surprise Creek, and forming the plateau upon 
 which the “ Quartz Hill Hotel” (Herberton and Georgetown Road) is situated, is a 
 highly vesicular basalt with immense geodes coated sometimes with calcite and sometimes 
 with silica. The basalt extends about a mile from the left bank of the creek. Mr. 
 Maitland has examined thin sections of this rock, and has furnished me with the 
 following note :— 
 
 “A specimen collected is of a dark greyish-blue colour, and somewhat porous and 
 vesicular. Scattered through it are yellowish grains of olivine, which often show a 
 beautiful iridescence on fresh fractures. Under the microscope the rock is found to be 
 made up of a granular mixture of felspar, augite, and olivine, with a little magnetite. 
 The felspar (plagioclase) occurs in long lath-shaped crystals, and is perfectly clear and 
 transparent. The crystals (which do not attain any great size) are remarkably free 
 from alteration. The augite occurs in crystalline grains, and is usually of a pale brown 
 colour, and exhibits faint dichroism. The olivine, which occurs porphyritically amongst 
 the other constituents, has almost always undergone a certain amount of alteration into 
 some ferriferous substance; generally the alteration is seen to commence along the 
 external boundaries of the crystals, and to extend gradually inwards along lines of 
 weakness. The magnetite, which is more easily detected with a magnet than under a 
 microscope, exists as small grains of every conceivable shape. In addition to these 
 constituents, there are long, colourless, acicular crystals of what appear to be apatite. 
 A fair quantity of glassy matter is discernible throughout the slice. A rock of this 
 character would be classed with the ‘ felspar-basalts.’ ”’ 
 
 Hinasleigh River.—Large sheets of basalt occupy the bed of the EHinasleigh 
 River and adjacent country where the river is crossed by the Pentland and Georgetown 
 Road, and also the valley of Spring or Lagoon Creek, near Carpentaria Downs Station, 
 and the Copperfield River where it is crossed by the same road. Lower down the 
 Einasleigh valley basaltic cowlées overlie alluvial deposits older than those of the recent 
 times, having been poured down the valley over the bed of the river, which at length 
 cut through, or found its way through past the edge of the basalt. 
 
 It was after the denudation of the Desert Sandstone of the Newcastle Range, which 
 overhangs the left wall of the valley, and subjacent rocks, had been carried on by the 
 Einasleigh for at least 1,000 feet that the lava-form basalts burst out and flowed down the 
 valley. Near the basalt a thermal spring, described in another chapter, shows that the 
 voleanic forces which produced the basalt, though diminishing, still possess some vitality. 
 
 The basalts overlying auriferous drifts on Kroombit Gold Field probably belong 
 to the New Volcanic series. Mr. Rands* thus refers to these basalts :— 
 
 “Small outliers of basalt overlie the Gympie Beds on the range dividing the 
 Kroombit and Three Moon Creek waters. A patch of basalt occurs about two miles 
 north-west of the township [Cania], and a small outlier is seen about three-quarters of a 
 mile south of Starlight Gully. The basalt is full of small blebs of olivine. 
 
 *Annual Progress Report of the Geological Survey for 1890, Brisbane: by Authority ; 1891, 
 20 
 
594: 
 
 “That the basalt is newer than the Desert Sandstone is shown by its level and 
 position. The Desert Sandstone once covered the whole of this district, and it must 
 have been removed by denudation before the basalt could have occupied its present 
 position. A large plateau of basalt occurs north of Cania Station, on the eastern side of 
 Spring Creek.” 
 
 The Basalt Wall which lies on the top of the older basalts of the Lolworth and 
 Dalrymple area is about fifty miles in length from west to east, and forms the highest. 
 land between Lolworth and Fletcher’s Creeks. 
 
 “Tt runs along in an east and west direction, at a distance of from two to six 
 miles north of Lolworth Creek. The basalt is highly seoriaceous. Everywhere the 
 cracks produced in the rock on cooling are visible, and there are immense spheroidal- 
 shaped masses in it, also produced by cooling. The lava must have outflowed ina 
 semi-viscous condition, for the well-known ‘ropy’ structure, formed by masses of 
 semi-liquid lava rolling over and over, is verv conspicuous ; this structure is easily seen, 
 even in hand specimens. The basalt consists of a groundmass of small felspar crystals, 
 with specks of augite (?) and magnetite. 
 
 “The basalt does not form a wall in the ordinary sense of the word—that is to 
 say, there are no perpendicular cliffs of it, but it gradually rises in steps, getting thicker 
 and thicker as it recedes from the margin. It is destitute of any vegetation, with the 
 exception of some plum and bottle trees and a few other scrub trees. I was informed 
 by Mr. Clarke, of Toomba, that he had discovered some miles of well-grassed open country 
 in the middle of this basalt. Its average breadth is about eight miles. Its general 
 appearance is that of a recent outflow of lava, and it probably represents the latest outflow 
 in the district.” * ; 
 
 It may be observed that many of the Newer Volcanic outbursts took place in 
 the neighbourhood of areas occupied by the Older Volcanic rocks, or actually overspread 
 the latter. Possibly the volcanic activity in some districts was continuous, but where 
 it is possible to distinguish between an older and a newer, the two may for the present 
 be kept apart. 
 
 Lithological observations on the basalts, &c., of this period will be found in the 
 notes by Mr. A. W. Clarke which accompany this work. 
 
 The late Mr. Daintree classed + with the Pliocene certain alluvial deposits 
 occurring at high levels above the Recent alluvia of the Cape River, which he thus 
 described :— 
 
 “Whilst the recent alluvial deposits seem only to reward the miner in the 
 immediate vicinity of some rich quartz reef or other gold matrix, this, so far as 
 yet tested, yields gold of a rounded waterworn character, independent of any 
 local source of supply. It differs from the first mentioned in the rounded character 
 of the contained pebbles, its interstratified white clays, and purer waterworn 
 gold. Isolated patches of this drift were observed from the head of the ‘Cape’ to 
 the ‘Lower’ diggings; what had probably at one time been a continuous line of 
 deposit having evidently been partially redistributed by the present watercourses. 
 At the junction of ‘Sandy Creek’ with the ‘ River Cape,’ a well-defined band of rounded 
 pebble-drift joins what may, for convenience sake, be called the ‘Main Lead;’ this 
 branch heads from the ‘Springs’ at ‘Talavera’s’ Camp, and keeps a course between the 
 Cape and Sandy Creek until it gains the so-called ‘Main Lead,’ as before mentioned. 
 Hence, following the line of ‘Gehan’s Flat,’ the ‘White Hills’ and ‘ Deep Lead’ (the 
 
 * Report on the Cape River Gold Field, by William H. Rands. Brisbane: by Authority : 1891. 
 + Report on the Cape River Diggings and the latest Mineral Discoveries in Northern Queensland. 
 Brisbane: by Authority : 1868, 
 
 
 
595 
 
 gold workings of which are all in this old rounded drift), there is no difficulty in tracing 
 similar material in cliff sections in a south-westerly direction, until it is no longer 
 confined within moderate limits, but opens out into a large marine or lacustrine deposit 
 to the south and south-east. 
 
 “On the accompanying map the extent of this particular Formation is shown 
 by the distinguishing colour ‘yellow’; and on reference it will be seen that down 
 the ‘Cape’ as far as the ‘Lower’ diggings, and down the ‘Running Creek’ at 
 far as the junction of ‘Golden Gully,’ it may be considered as the representative 
 of old-river channels; beyond these points to the south and east it can be regarded 
 in no other light than that of accumulated sediment from a vast lake or sea. 
 It has been found in working that where this supposed old watercourse is narrowest, 
 as at ‘Gehan’s’ Flat, ‘White’ Hill, &c., there the gold is most concentrated; but 
 when it becomes broader, and the drift deeper, as on the extension of the ‘ Deep 
 Lead’ to the south, the gold is found to be too scattered to pay for the additional cost 
 of mining.” 
 
 Of these drifts, Mr. Rands observes * :—‘ Several alluvial leads of older date 
 than the alluvium of the present watercourses occur, and have been worked for gold. 
 They consist chiefly of a schistose drift, with a ‘wash’ of coarse quartz pebbles at the 
 bottom, and are evidently the drift of old watercourses. Some of them have given 
 splendid returns of gold. The principal ‘lead’ is one running south from the Lower 
 Cape, which averaged about 3 ozs. of gold to the load for about two miles in length. 
 The depth of this drift varied from three feet to one hundred feet. It got wider and 
 deeper towards the south. The gold was much waterworn and rounded. Leads of very 
 similar character occur on the opposite side of the Cape River, at the Lower Cape, and 
 also up Sandy Creek, near Chinaman’s Gully. The Canton and Pothole Leads, at the 
 Upper Cape, have also given handsome returns.” 
 
 The late Mr. D’Oyly H. Aplin, evidently inclined to consider the “‘ Older Alluvial” 
 of the Gympie Gold Field as the equivalent of the Victorian Pliocene, says +:——“ A 
 stratified quartz pebble drift of older date than the existing valleys, and of which the 
 remains now occupy the summit of ridges skirting these valleys. It is well shown 
 capping a series of ridges on the west side of the One-mile Creek, about two and a-half 
 miles above its junction with the River, in a large ‘pocket’ of the creek known as 
 Macpherson’s Paddock. It forms also a conspicuous feature on the west side of the 
 Six-mile Creek, near the crossing of the road, about seven miles above Gympie; and has 
 doubtless at a former period extended over a considerable area of the valley now 
 occupied by the Mary and its tributaries. It consists almost entirely of rounded and 
 waterworn quartz, varying in size from small gravel to boulders upwards of one foot in 
 diameter, and intermixed with sandand clay. Associated with it are beds of ferruginous 
 quartz conglomerate. These deposits are precisely similar in appearance, character, and 
 position to those which constitute the ‘ made hills’ of many of the Victorian goldfields, 
 and which have there proved to be highly auriferous. They appear to have been 
 almost entirely neglected or overlooked here, but are well worth the attention of 
 prospectors, as the discovery of alluvial leads in the adjacent valleys would probably 
 follow should the result of prospecting amongst these ‘made hills’ prove successful, 
 The gold, if any, would be in a smooth, waterworn state, and entirely free from 
 quartz—in this respect, unlike that obtained from the shallow gullies in the vicinity of 
 the reefs.” 
 
 * Annual Progress Report of the Geological Survey for 1890. Brisbane: by Authority: 1891. 
 t+ Report on the Geological and Mining Features of the Gympie Gold Field. Brisbane: by Authority: 
 1868, 
 
596 
 
 Of the Gympie drifts, Mr. Rands writes as follows * :— 
 
 “ An alluvial deposit occurs in many parts of the district of an older date than 
 the deposits being formed by the existing streams. It consists chiefly of a drift of large 
 waterworn pebbles, varying in size from half-an-inch to eight or more inches in 
 diameter, the pebbles consisting of quartz and of hardened jasperised sandstone. 
 There are also layers of ferruginous grit and conglomerate. 
 
 “This older alluvium can be seen in many places in the western side of the 
 river; on some ridges on the western side of Deep Creek, about three miles from its 
 mouth; near the Brisbane road on the Six-mile Creek; to the north of Gympie 
 patches of it are met with here and there for the whole of the distance to Maryborough. 
 Close to Maryborough, in the Tinana Division, a shaft that was sunk on a ridge passed 
 through some thickness of this drift, and gold was found in one or two of the pebbles 
 on their being broken. 
 
 “There is another alluvial deposit, probably of still earlier date, which forms a 
 capping to the One-Mile (Red Hill) and Surface Hills in Gympie. This deposit 
 consists of yellow and red stratified sandy and aluminous silts, with, in places, masses 
 of pebbles and boulders of quartzite, which are well shown in the new railway cutting 
 on the north side of Red Hill. There is no evidence as to the exact age of these deposits, 
 beyond that they are newer than the reefs in the Gympie Beds below, as they are not 
 intersected by them. A little waterworn gold has been found on parts of Red Hill; 
 and on Surface Hill, in the Channon-street cutting, small nuggets of gold have been 
 picked up. Small prospects of gold are nearly always obtained on working the soil on 
 Surface Hill.” 
 
 The Upper and Older Alluvia of the Stanthorpe tin-mining district are probably 
 contemporaneous with similar drifts on the New England side of the border, which 
 Mr. David classes as Pliocene. 
 
 It is quite possible that the Cape, Gympie, and Severn, and many other ancient 
 alluvial drifts may turn out to be Pliocene, but at present we have no direct evidence to 
 enable us to distinguish them from Post-Tertiary drifts. They probably never were 
 covered by basaltic lavas, as any erosive agent capable of denuding the latter would in 
 all likelihood have cleared away the underlying incoherent drifts also. 
 
 In my opinion the drifts of the Severn Valley point to a period of heavy 
 rainfall, accompanied probably by the occasional melting of snow. A somewhat more 
 rigorous climate than the present probably prevailed, but a careful search failed 
 to reveal striated stones or anything indicative of a true glacial period. 
 
 Mr. Henry G. Stokes, who has collected near Oxley a number of beautifully 
 preserved plant remains, which have been submitted to Professor Baron Von 
 Ettingshausen for determination, has kindly given me the following notes “On the 
 Occurrence of Tertiary Beds in the neighbourhood of Brisbane” :— 
 
 “Between Sherwood and Wolston stations, on the Ipswich Railway Line, and 
 extending for some distance to the south-south-east of Sherwood, a series of beds occurs, 
 consisting of pale and yellow-coloured, coarse and fine grained, argillaceous and 
 ferruginous sandstones, sandy shales, and clays. 
 
 “The principal rock in .this series is a pale-coloured variety of sandstone, 
 consisting of an abundance of small angular and sub-angular quartz grains, and white 
 mica, with clay, and a little oxide of iron and carbonate of lime as the cementing 
 material. It is not a very coherent stone, and, with the exception of those portions in 
 proximity to an intrusive rock, weathers rapidly on. exposure. 
 
 
 
 * Report on the Gympie Gold Field. Brisbane; by Authority : 1889. 
 
597 
 
 “Numerous cracks and joints divide the rock into small, rough prisms; and 
 especially is this the case in the neighbourhood of the basaltic rock, where the sandy 
 shales have seemingly separated into rough spheroids. The beds are traversed by a 
 number of small faults, striking S.E.,S8.S.EH., and 8S. 10 E., the largest displacement 
 noticed not exceeding eight feet. 
 
 ‘As by far the greater portion of the formation is covered by alluvium, the dip 
 of the beds and strike of the faults and joints can alone be noticed in a few localities, 
 and where they have been exposed by denudation the bedding planes are not sufficiently 
 defined to allow of accurate measurements being taken The beds are generally 
 horizontal, undulating slightly, and where they are inclined they dip at varying angles. 
 
 “In Mr. De Winton’s paddock, Corinda, adjoining the river bank, this series, 
 which is there horizontal, is seen resting unconformably on a series of coarse, gritty 
 sandstones and conglomerate, belonging to the so-called Ipswich Beds. 
 
 “These Tertiary deposits occupy a considerable portion of the depression, 
 extending from Sherwood, on the Southern and Western Railway Line, to beyond 
 Runcorn Station, on the Logan Line. Outcrops of the coarse grits and conglomerates, 
 apparently of a different geological age, occur in several places, rising above the level of 
 the valley, forming extended ridges and hillocks. 
 
 “‘ Most of these beds contain monocotyledonous and dicotyledonous plant remains, 
 which may be referred to some period of the Tertiary epoch. In the shales and clays, 
 the venation of the leaves and stems of the plants are sharply defined, and their 
 outlines well marked in the remaining beds, but few of the impressions are well 
 preserved, their exterior outlines being with difficulty discernible.” 
 
 I have gone over the section ecarefuliy, and can see no marked lithological 
 distinction between the strata from which Mr. Stokes obtained his fossils and many 
 other well-known beds which unquestionably form part of the Ipswich Coal Measures ; 
 nor can I see any evidence of an unconformability of more importance than many local 
 unconformabilities which occur in the Ipswich Beds. I should incline to regard Mr. 
 Stokes’ fossils as additions to the flora of the Ipswich Formation rather than as evidence 
 of the presence of Tertiary strata. The whole question can, however, remain in 
 abeyance pending Baron von Ettingshausen’s determination of the fossils. 
 
 MINES IN CONNECTION WITH THE TERTIARY ROCKS. 
 RUSSELL RIVER GOLD FIELD. 
 
 This is a recently opened alluvial. field which is likely to rise into importance. 
 Its centre is about six miles west of Mount Bartle Frere. The gold is found associated 
 with fine-grained stream tin ore in a gravelly wash beneath basaltic flows, about 2,500 
 feet above the sea-level. This basalt forms part of the tableland which extends from 
 the heads of the Russell, Johnstone, and Mulgrave to the basin of the Barron near, 
 Herberton, and is covered with dense tropical jungle and intersected by plentiful 
 running streams. It probably dates from Miocene times, but of this no direct evidence 
 has yet been observed. Wairambar Creek, on the west, and Cooppooroo Creek, on 
 the east, have cut through the basalt, exposing the underlying auriferous drift and 
 the “bedrock” of slates, schists, and greywackes. Extensive preparations for sluicing 
 the drifts have been made, and as the area covered by the basalt is enormous, and the 
 drift has been exposed, owing to the accident of denudation, merely on the fringe of the 
 deposit, almost unlimited possibilities are before the field. The average yield from 
 washdirt reported in Victoria for 1883 was 1 dwt. 23°32 grains; for 1884, 3 dwts.; and 
 for 1885, 1 dwt. 10°59 grains. I am certain that the Terraces of the Russell will give a 
 
598 
 
 much higher yield than this, and there is no comparison between the extent of the 
 auriferous areas of Victoria and those of the Russell. The Wardens have been unable 
 to form any estimate of the alluvial gold from this field. 
 
 Gold and stream tin ore are found in the beds and alluvial flats of the Lower 
 Russell and the Johnstone. No reefs of any importance have yet been worked in the 
 district, and it is probable that the alluvial gold has been mainly derived from the 
 denudation of the drifts beneath the basalt. There is, however, a rumour of a rich 
 reef having been lately discovered. 
 
 MULGRAVE GOLD FIELD. 
 
 For remarks on alluvial workings, see Chapter XIII. 
 
 MOUNT MORGAN GOLD MINE. 
 
 This mine, which has already (up to 3lst December, 1891) produced 907,697 
 ounces of gold, is not only one of the richest in the world, but presents geological features 
 of unusual interest. It lies about twenty-six miles south-south-west of Rockhampton. 
 
 In the immediate neighbourhood of the mountain, the country-rock consists 
 mainly of bluish-grey quartzite—a fine-grained siliceous sandstone, now more or less 
 porcellanised—full of minute crystals of iron pyrites and specks of magnetic iron ore; 
 greywackes of the ordinary type—hard fine-grained sandstones of mingled siliceous 
 and felspathic materials, now somewhat indurated; and, lastly, occasional masses of 
 pyritous shale, hardened to a flinty consistency, and a few belts of serpentine. These 
 sedimentary rocks have been shown, from a large collection of fossils made by the late 
 Mr. James Smith, to belong to the Gympie Formation. In the immediate neighbour- 
 hood of the Mount the sedimentary rocks appear to have been in thick beds, and they 
 have suffered a considerable amount of metamorphism, so that their dip and strike are 
 not easily ascertainable. The stratified rocks are, moreover, interrupted and inter- 
 sected in every direction by dykes and other intrusive masses of hornblendie granite 
 and porphyritic dolerite,* the intrusive masses occupying nearly as much space as the 
 remnant of the original stratified formation itself. The country-rock within a short 
 distance of the Mount is traversed by reefs of the ordinary description, such as, for 
 instance, the Golden Spur Reefs, the Crow’s Nest Reef, and the Mundic Reef, all of 
 which contain a pretty fairamount of gold. 
 
 The Mount is about 1,200 feet above the sea-level, or about 500 feet above the 
 level of the Dee River, which flows past its eastern foot. The “ mine’’ presents the 
 appearance of a series of step-like quarries at different levels. The actual summit of 
 the mountain has now been bodily quarried away to a depth of thirty-five feet, the 
 level of the Second Floor.+ Numbers 3 and 4 Floors are respectively thirty-five and 
 seventy feet below the level of No. 2; and No. 5 Floor is thirty-five feet below No. 4. 
 What is called the Crown Shaft or Main Pass is sunk from the second Floor to a depth 
 of 155 feet, beneath No. 5 Floor. No. 2 Tunnel is driven right across the hill from 
 north to south at the level of No.5 Floor. No.1 Tunnel, a little more to the west of 
 north and east of south, is driven across the whole of the auriferous area one hundred 
 and fifty-five feet below the level of No.2 Tunnel, while the Freehold Tunnel is driven 
 from east to west thirty-three feet above No.1 Tunnel. The Sunbeam Tunnel is carried 
 
 * See Notes on a Collection of Rocks and Minerals from Mount Morgan, collected by Mr. C. 8. 
 Wilkinson, F.G.8., &c. ; by T. W. Edgeworth David, B.A., and William Anderson, Geological Surveyors. 
 With an introduction by C. S. Wilkinson, Geological Surveyor in Charge. Records of the Geological 
 Survey of New South Wales, ii., p. 85. Sydney: by Authority : 1891. 
 
 + Now (June, 1892) mainly to the level of No. 4 Floor, 
 
 atl sie ate 
 
599 
 
 from the south-west nearly to the Crown Shaft, and the Grass-tree Tunnel (about 
 seventy feet below the level of the Freehold Tunnel) is driven from the south-east to 
 the Crown Shaft.* 
 
 The upper portion of the mountain consists of a deposit varying from red and 
 brown hematite on the one hand to a frothy, spongy, cellular, siliceous sinter on the 
 other. Fine gold is disseminated throughout the mass, but it varies considerably in 
 richness. So far as the upper excavations show, the auriferous deposits are bounded to 
 the south-west by a large kaolinised granitic dyke, but on No. 8 and No. 5 Floors the 
 dyke intersects the auriferous deposits, some portion of the latter being found on its 
 south-west side.t At the eastern end of the auriferous deposit, on the other hand, there 
 are immense quantities of kaolinised rock, “rich in gold—z.e., from }-0z. to 22 ozs. to 
 the ton.” (Manager’s Report, Ist June, 1891.) No. 1 Tunnel discloses immense 
 quantities of highly pyritous quartzite country-rock. Indeed, there is more pyrites than 
 quartzite. 
 
 Possessing (as will be seen from any plan of the workings) none of the 
 characteristics of a “reef,” as the term is generally understood, it becomes necessary 
 to seek for another explanation of the origin of the auriferous deposit. I am of opinion 
 that the gold must have been precipitated in the ferruginous and siliceous sinter 
 deposited by a thermal spring, which, charged with chlorine, dissolved the gold from the 
 pyrites of such reefs as the “ Mundic Reef,” and from the pyrites with which the 
 country-rock beneath and around the summit of the Mount is abundantly charged. 
 Even if the gold was present in the pyrites of the country-rock in a very infinitesimal 
 proportion, it might be collected by a thermal spring from such pyrites over a wide 
 area. 
 
 The occasionally angular condition of the sinter, and the tumbled condition of 
 the ironstone masses (as evidenced by the deflection of stalactites from the vertical) 
 would appear to indicate that explosive discharges of gases or steam occurred at 
 intervals with sufficient violence to disturb the deposits accumulated by the thermal 
 spring. 
 
 Mr. A. W. Clarke, of Charters Towers, late Government Mineralogical Lecturer, 
 has favoured me with the following Note on some specimens from Mount Morgan :— 
 
 “‘ A very large proportion of the substance is soluble in strong potash solution, 
 the residue being nearly pure crystalline silica. This is what ought to be expected of a 
 siliceous sinter, as, of course, the silica would be hydrated and colloidal, and the presence 
 of some quartz (or crystalline silica) in it is quite conceivable.” 
 
 Mr. Walter H. Weed, of the United States Geological Survey, who has made a 
 special study of the wonders of the Yellowstone National Park, writes me ¢ as follows:— 
 “The specimen of sinter which you enclosed is too small for satisfactory examination. 
 It bears a striking resemblance to certain rhyolitic pumices from the Yellowstone, but 
 lacks porphyritic crystals, while your observations regarding its occurrence render such 
 an origin impossible, while another proof is easy in complete analysis. The sinter is 
 not quite like anything in our collection from the Yellowstone, Iceland, or New Zealand 
 districts. It appears, however, to be a good sinter, and its vesicular or frothy nature 
 indicates that it was formed at the surface. As to Mr. Cameron’s remarks (quoted on 
 p. 5 of your Report of 1889), his objection to the thermal spring theory, based on the 
 
 * An account of later workings and developments will be found in the Writer’s ‘‘ Third Report on the 
 Mount Morgan Gold Deposits.” Brisbane: by Authority : 1892, 
 
 + This is also the case in the ‘‘ Freehold Stopes,’ a few feet above the level of the Grass-tree Tunnel, 
 Sce ‘‘ Third Report.” , 
 
 t In a letter dated 27th November, 1889, 
 
600 
 
 absence of calcareous tufa, is quite erroneous. Hot waters issuing from voleanic rocks 
 usually deposit siliceous sinter, and that alone, the lime being carried off in solution by 
 the waters, and usually present in very minute quantity. Calcareous deposits under 
 such circumstances are rare exceptions,* and not the rule. The facts described in your 
 Report seein to offer conclusive evidence in favour of your theory.” 
 
 As has already been mentioned, numerous dykes of diabasie dolerite + intersect the 
 country-rock. Not one, however, is met with in the auriferous deposit. Had the latter 
 been merely the siliceous skeleton remaining after the removal of the pyrites from the 
 pyritous quartzite, the dolerite dykes would still be present to attest the original identity 
 of the two masses. But there is at least one clear instance of a dolerite dyke intersecting 
 the quartzite country-rock (in No. 1 Tunnel, one hundred and twenty feet north of the 
 shaft sunk from No. 5 Floor) and not intersecting the overlying sinter (in the south 
 branch of the Freehold Tunnel, only thirty-five feet higher) ; showing tbat the sinter 
 and ironstone were deposited on, and were not altered portions of the pyritous quartzite 
 country-rock. It is hardly credible that the highly auriferous siliceous and ferruginous 
 material now being worked represents merely a weathered condition of the pyrites with 
 which the quartzite country-rock is so highly charged, and which is so poor in gold. 
 Again, the fact that the sinter is mainly a hydrous silica is an argument against its being 
 the skeleton produced by the solution of masses of pyrites from an anhydrous quartzite. 
 
 For some distance around the Mount, the country-rock is frequently impregnated 
 with aluminous, siliceous, and ferruginous material. Some portions of this rock were 
 so far gone that on my first visit to Mount Morgan (1884) I imagined them to represent 
 deposits from the overflow of the thermal spring, an idea which I have since abandoned, 
 although it is likely enough that the influence of the thermal spring may have assisted in 
 the decomposition of the adjacent rocks for some distance, and some of the easily soluble 
 mineral matter may have percolated into the superficial portions of the adjacent rocks. 
 
 The gold of Mount Morgan is probably the purest that has ever been mined. 
 Dr. A. Leibius, of the Sydney Mint, says it assays as high asy99°7 per cent. The gold 
 is extracted by a process of chlorination, but its recovery from the recently discovered 
 “kaolin ores’’{ has proved to be a much slower process than its extraction from the 
 siliceous and ferruginous. 
 
 My reasons for classing the Mount Morgan Gold Mine as Tertiary are the 
 following :— 
 
 ‘That the deposit left by the thermal spring is newer than the altered stratified 
 rocks through which it has burst is obvious; and that it is even newer than the much 
 later date when the dolerite dykes filled up fissures in the stratified rocks, is proved by 
 the fact that the dykes are clearly seen in some instances to be covered over by the 
 siliceous, aluminous, and ferruginous deposits of the spring. 
 
 “But yet another circumstance helps us in our endeavour to ascertain the age 
 of the outburst of the Mount Morgan hot spring. About a mile to the west of the 
 ‘mountain’ is a mass—apparently about one hundred and fifty feet in thickness—of 
 horizontal bedded sandstone, undoubtedly the ‘ Desert Sandstone.’ It rests, apparently, 
 at this point, on a mass of diabase, but in other places it may be seen lying on the 
 upturned edges of quartzite and greywacke strata, similar in character to those of the 
 ‘country’ around Mount Morgan. The base of this Formation is a fine volcanic dust. 
 
 The upper beds are coarsely gritty, and for the most part siliceous, varying from white. 
 
 * The Einasleigh Thermal Spring is one of the exceptions. See Chapter xxxvi. 
 
 t See Notes by Messrs. Edgeworth David and Anderson above quoted. 
 
 } The kaolin of these ores, I understand, rarely exceeds thirty per cent, of the whole, the remainder 
 being siliceous sinter. 
 
601 
 
 to brown and red, and containing occasional pebbles of quartz and quartzite. The base 
 of the Desert Sandstone I should judge to be about a hundred feet lower than the 
 summit of Mount Morgan. 
 
 “ Standing on fits sandstone cliffs, so as to look to the east, past the south side 
 of Mount Morea the observer can descry, across the valley of the Dee, the familiar 
 contour of horizontal-bedded sandstone cliffs stretching North and South. As nearly 
 as can be judged by the eye, they are on the same level as the cliffs on the opposite side 
 of the valley, and there can be no doubt that the valley has been carved out of a once- 
 continuous cake of horizontal sandstone. The question arises, ‘Was Mount Morgan 
 an island in the sea or lake in which the sandstones were laid down?’ In that case the 
 hot spring was older than the Desert Sandstone. 
 
 “The answer is easily made. Had there been shores to this sea or lake where 
 Mount Morgan now stands, the sandstone in the neighbourhood would have been full of 
 pebbles of sinter and ironstone derived from the waste of such easily degraded rocks. 
 But I saw none such, and I believe they do not occur. The hot spring, then, was newer, 
 and not older, than the Desert Sandstone.”’* 
 
 In many localities in the North, as may be seen in previous portions of this 
 Chapter, the valleys carved out of the Desert Sandstone became the theatres of voleanie 
 activity, represented by flows of basaltic lavas and “foci” filled with ash or basalt 
 and in some instances by crater-shaped hills. Another form of volcanic activity was 
 developed at the same period near the head of the Dee Valley. After the Desert, 
 Sandstone had been uplifted, and the carving-out of the present valleys had been carried 
 on for long ages—in fact, till the valleys had nearly acquired their present contours— 
 basaltic lava flowed down the valleys over the upturned slates of the MacIvor and over 
 the auriferous drifts of the Mulgrave, and a thermal spring of enormous proportions 
 burst out, or perhaps even a geyser spouted fitfully in the valley of the Dee, carrying 
 with it not only water, but in all probability chloride of gold. 
 
 The literature of Mount Morgan is already apleinane The reader may 
 consult — 
 
 (1.) Lzrerus, A—Notes on Gold. Journ. R. Soc. N.S. Wales for 1884 
 [1885], xviii., p. 37. 
 
 (2.) Grecory, A. C.—Observations on the Occurrence of Gold at Mount 
 Morgan. Proc. R. Soc. Queensland, 1884. 
 
 (3.) Jack, R. L.—Report on the Mount Morgan Gold Deposits. Brisbane: 
 by Authority: 1884. 
 
 (4.) ZId.—Second Report on the same. Brisbane: by Authority: 1889. 
 
 (5.) Macponatp Cameron, J.—Report on Mount Morgan, to the Directors, 
 dated 26th March, 1887, reprinted in Rockhampton Bulletin. 
 
 (6.) Ricxarp, T. A. (of California).—Mount Morgan Mine. Articles in 
 Melbourne Evening Standard for 183th and 14th March, 1890. 
 
 (7.) Sykes, Writt1am H.—A Practical Treatise on Mount Morgan. Mount 
 SMa ian Chronicle Office, 1888. 
 
 (8.) Witxtnson, C. S.; Davin, T. W. Enegewortu ; and AnpERsoN, WIL- 
 11AM.—Notes on a Collection. of Rocks and Minerals from Mount 
 Morgan, already quoted. (See page 598.) 
 
 (9.) Mine Sections and Working Plans issued by the Directors, July, 1890. 
 
 (10.) Jack, R. L.—Third Report on the Mount Morgan Gold Deposits. 
 Brisbane: by Authority: 1892. 
 
 * Report (First) by R.L.J. on the Mount Morgan Gold Deposits, Brisbane: by Authority: 1884, 
 
602 
 
 MOONDILLA GOLD FIELD. 
 
 Although widely different in its physical aspects, this Goldfield belongs, I am 
 fully persuaded, to the same category as Mount Morgan, representing another phase of 
 the activity of thermal waters, probably manifested at or about the same period of time. 
 
 The “ Goldfield” occurs on the dividing line between Gumbardo and Milo Runs, 
 in the middle of nearly dead-flat mulga-covered pastoral land. What may be called the 
 -“bed-rock” of the district is the “ Rolling Downs” or “ Lower Cretaceous” strata, which 
 have already been described. This is covered by the material about to be described, 
 and which can be identified as derived from the debris of the Upper Cretaceous or 
 Desert Sandstone, of which denuded fragments occur in the neighbourhood. 
 
 The groundwork of the field consists of what is known as “cement,” a some- 
 what consolidated ‘‘wash” of materials for the most part siliceous, but to some 
 extent felspathic. This cement, on being broken up and washed, is found to contain a 
 considerable quantity of hydrous silica, which is not in rounded waterworn grains, but 
 in concretions or nodules. Sometimes the silica, when present in large quantities, forms 
 lenticular concretionary masses, and even what may be called beds, strata or seams 
 interstratified with the cement. When these beds attain any thickness they present 
 almost every variety of the chalcedony group of hydrous silica, varying in colour from 
 smoky to yellow, pearly, milk-white, and water-clear, and, while breaking with great 
 facility (with a conchoidal fracture) into “knives’’ or “ flint-flakes,” can be seen on 
 every surface and in every thin section to have a nucleated structure throughout. 
 
 The above characteristics, and above all its low specific gravity, would enable any 
 miner to distinguish this from the auriferous stone of any hitherto known goldfield. 
 The low specific gravity is, of course, due to the fact that water enters into its 
 composition, so much of it as is water being only two-fifths of the weight of an equal 
 bulk of common anhydrous quartz. 
 
 If it be permissible mentally to reconstruct the conditions under which the 
 Goldfield was created, we may imagine, in the first place, a land surface on which the 
 Upper Cretaceous (Desert Sandstone) lay on the Lower Cretaceous (or “ Rolling 
 Downs”) strata. In course of time the Desert Sandstone was denuded till mere 
 fragmentary tablelands of it remained in sitw, the débris of the portion removed being 
 spread over the surrounding low country. From abundant evidence furnished by other 
 parts of Australia, it is known that at a period (Newer Tertiary ?) when the denudation 
 of the Desert Sandstone had gone on for some time, immense outbursts of volcanic 
 activity took place, giving rise in some cases to flows of basaltic lava, and in others to 
 fountains of warm water. We may presume that the latter was the case at Moondilla, 
 and that the water was highly charged with dissolved silica, of which it carried quantities 
 into the then loose and incoherent masses of débris formed of the waste of the Desert 
 Sandstone. The silica, at first ina gelatinous condition, would eventually be segregated 
 into concretions surrounding nuclei or filling up spaces or openings in the bedding- 
 planes, and on consolidating and crystallising would have no difficulty in elbowing 
 portions of the cement matrix out of the way and assuming the gnarled and twisted 
 forms presented by the majority of the concretions and seams. In all probability the 
 thicker beds of silica represent pools of silica-charged water, which were ultimately 
 covered up by further accessions from the débris of the Desert Sandstone. With the 
 silica a limited amount of gold appears to have come up in solution, and to have been 
 deposited with it, possibly precipitated by the agency of sulphate of iron. The portions 
 of the silica richest in gold are those which are seamed with iron oxide. 
 
 The silica occurring in the cement has evidently hada similar origin to that which 
 forms comparatively thick beds. It is not waterworn, and has not been carried by 
 
 
 
 | 
 | 
 
603 
 
 running water, but is concretionary—the result of the segregation, around nuclei, of a 
 certain amount of the same material, once more widely disseminated throughout the 
 surrounding mass. There is no reason to suppose that the gold, any more than the 
 silica, was carried from a distance, or emanated from any reef which may be discovered 
 by trenching or sinking. 
 
 The following, from a trench in “No. 1 East”? Claim, may be taken as a typical 
 section:—1, Red soul, 1 foot; 2, Silica, 1 foot; 3, Cement, with bands of silica, 3 
 inches ; 4, Cement, with horizontal lines of cavities, a yellowish stain, and small 
 concretions of silica, 1 foot 8 inches; 5, Silica, 0 to 3 inches; 6, Same as No. 4, 
 10inches ; 7, Cement, with bands of silica, sometimes coming together into a thick bed, 
 1 foot 3 inches. 
 
 The silica beds sometimes attain a thickness of three feet, and in some cases thin 
 out rapidly, so that it would be impossible to say, without continuous working, whether 
 beds seen in shafts a few yards distant are identical or not. On the “Range” (an 
 almost imperceptible rise, perhaps six feet above the general level of the flat), the first 
 silica bed is generally met with within three feet of the surface ; but some shafts have not 
 met any thick bed. The deepest shaft, when I visited the place in company with Major 
 Moore, the Warden for the District, in September, 1891, was fifteen feet. 
 
 Before I left Brisbane for Moondilla, I was permitted to see a parcel of 
 specimens, apparently rich in gold. The stone was unquestionably of the same unusual 
 character as that which I subsequently saw stacked in large quantities on the Field 
 itself, although in the latter I could detect no visible gold. After much careful 
 pounding and washing, a very few “colours” were, however, obtained. It is now said 
 that the specimens exhibited in Brisbane had fine gold ingeniously plastered on them. I 
 retained only one of the Brisbane specimens, showing a minute speck of gold, and the latter, 
 after the lapse of ten months, has disappeared. I have been unable to obtain a sight of 
 the other specimens. There can be little doubt that the short-lived “ Moondilla rush” 
 was the result of a rascally case of “salting.” The visit of inspection had the effect of 
 preventing further mischief, as the Warden agreed with me that the “ prospects” did 
 not warrant the proclamation of a Goldfield. 
 
 The Moondilla country is, in ordinary seasons, a very dry one, but, the geological 
 conditions being favourable to the discovery of artesian water, infinite possibilities of 
 profitable working are open should payable gold be found. Even as it is, I consider 
 that the discovery of gold although in minute quantities must attract attention to the 
 presence of the precious metal under conditions which are certainly new, and which 
 may yet prove to be of importance, as a similar formation to that of Moondilla is 
 reported to cover extensive areas in the West. 
 
 J. 
 
CHAPTER XXXVI. 
 
 POST-TERTIARY AND RECENT. THERMAL AND OTHER SPRINGS. 
 
 STANNIFEROUS DRIFTS, VIZ.: STANTHORPE, MOUNT SPURGEON, AND PASCOE TIN 
 FIELDS. 
 
 Sir Thomas Mitchell, in January, 1842, sent to England some specimens of 
 Diprotodon “from the Condamine River, in Lat. 28° S., Long. 150° EH.” It is 
 evident that the Latitude and Longitude are wrong, and Mr. George F. Bennett 
 concludes * that the part of the river’s course referred to must be between Leyburn 
 and Yandilla. 
 
 Leichhardt is quoted by Mr. Bennett + as having written, apropos of some fossils 
 sent home by him on 10th July, 1844, from the Darling Downs :—“ The plains are filled 
 by an alluvium of considerable depth, as wells, dug fifty to sixty feet deep, have been 
 sunk within it. The plains and creeks in which fossils have been found are—Mr. 
 Hodgson’s Creek, Campbell’s Creek, Mr. Isaacs’ Creek [Gowrie Creek], and Oakey 
 Creek. They pass all into and through immense plains on the west side of the 
 Condamine, into which they fall. The bones are either found in the bed of the creek, 
 particularly in the mud of dried-up waterholes, or in the banks of the creek, in a red 
 loamy breccia, or in a bed of pebbles, containing many trachyte pebbles from the Coast 
 Range, from the west side of which these oak descend.” 
 
 In his “ Journal,” Leichhardt wrote { in the end of September, 1844:— 
 
 “We passed the stations of Messrs. Hughes and Isaacs, and of Mr. Coxen, and 
 arrived on the 80th September at Jimba [Jimbour?], where we were to bid farewell to 
 civilisation. 
 
 “These stations are established on creeks which come down from the western. 
 slopes of the Coast Range . . . and meander through plains of more or less extent 
 to join the Condamine River. . . . These plains have become remarkable as the 
 depositaries of remains of extinct species of animals. : 
 
 “Mr. Isaacs’ Station is particularly rich in these fossil remains ; and they have like- 
 wise been found in the beds and banks of Mr. Hodgson’s and of Mr. Campbell’s Creeks, 
 and also of Oakey Creek. At Isaacs’ Creek [Gowrie Creek] they occur together with 
 Recent freshwater shells of species still living in the neighbouring ponds, and with marly 
 and caleareous concretions, which induces me to suppose that these plains were covered 
 with large sheets of water, fed probably by calcareous springs connected with the 
 basaltic range, and that huge animals, fond of water, were living either on the rich 
 herbage surrounding these ponds or lakes or browsing upon the leaves and branches of 
 trees forming thick brushes on tke slopes of the nie bonnet hills. 
 
 Mr. George I. Bennett (son of Dr. George Bennett, of Sydney, and an enthusiastic 
 naturalist and collector of Darling Downs fossils), in the Paper above referred to, gives 
 the following notes :— 
 
 “The bank of Gowrie Creek, from the Gowrie Junction Railway Station until it 
 goes into Westbrook Creek, is more or less rich in fossils. The portion from the 
 
 
 
 * Notes on Rambles in Search of Fossil Remains on the Darling Downs. [1876.] Queensland 
 Philosophical Society’s Annual Report for 1877. 
 
 + Loc. cit. 
 
 +t Journal of an Overland Expedition in Australia, p. 1. London, 1847. 
 
 
 
 
 
 
 
 
 
 
 
605 
 
 junction to the Railway Bridge, Dalby Line, has only had a few stray bones found in it, 
 as the black soil there is very deep, and, in my opinion, the strata containing the fossils 
 are only just now becoming exposed; but from thence to the boundary of Gowrie is 
 very rich. 
 
 “ To return to the consideration of the localities in which fossil remains are to be 
 found, I think I can put the boundaries pretty well from Gowrie to Spring Creek, 
 Chfton (none are recorded as being found in Dalrymple Creek, on the Warwick side of 
 Spring Creek) ; thence to the Condamine River, and along its eastern bank as far as 
 Chinchilla (where I have seen specimens embedded in the rock). These boundaries 
 include Eton Vale, Clifton, Pilton, Gowrie, Yandilla, Cecil Plains, St. Ruth, Jimbour, 
 and Warra Warra, Jimbour Station being the northern boundary.”’ 
 
 Mr. Samuel Stutchbury refers * to “the cementation of drifted matter [on 
 the Darling Downs] such as pebble, shingle, frequently containing fragments of the 
 bones of extinct animals, many of them being much abraded by rolling, whilst others, 
 together with the exuvia of fresh-water mollusks of existing species (the Unios only 
 differing from their having attained a larger size and thickness), are found drifted 
 together with little or no injury, and cemented by calc-sinter, calcareous tufa, 
 and travertin.” He adds: “ Bones have been found at all the various depths at 
 which the alluvial soil of the plains has been penetrated, even from wells at a 
 depth of sixty or more feet, as was the case in sinking a well at Nombi, on the 
 Liverpool Plains; therefore, the race of animals now extinct must have existed 
 throughout the period of time necessary for the accumulation of the vast amount of 
 alluvial drift; or the drift must have undergone many mutations, by being swept away 
 and being redeposited.” 
 
 In a later Report + Mr. Stutchbury mentions the following localities from which 
 bones of extinct animals have been obtained :—King’s Creek, Emu Creek, Hodgson 
 Creek, Clifton, Gowrie Creek, Myall Creek, Bowra Creek, and Dalby. From this 
 Report the following stratigraphical notes are taken :— 
 
 “King’s Creek presents a succession of waterholes, circular, oval, and linear, and 
 exhibits on the banks, by successive layers of shells, distinct periods of deposition ; this 
 is particularly apparent near Clifton, the bed of the creek being composed of a peculiar 
 conglomerate made up of débris containing shells, bones, &c., and cemented with lime; 
 fossil trunks of coniferous trees upon the same level were observed in situ as if cleanly 
 sawn ; above this the deposits of different periods may be clearly traced.” 
 
 “Crossing Gowrie Creek, I proceeded to the junction of Oakey and Pitt’s Creek 
 with Westbrook Creek; the banks in many instances exposed a reddish marble 
 containing calcareous tufa and fragments of bone. 
 
 *¢T was shown at Dalby the jaw of a wombat (Phascolomys Mitchelli) and other 
 larger bones, obtained at a depth of sixty feet from the surface while sinking a well. 
 The fact of bones being found at such depths, while in other places they are near the 
 surface, would, at first sight, appear to be evidence of their having existed throughout 
 the period of time necessary for the deposit of sixty or more ie of alluvial matter. 
 This, I presume, is not the case, but that their being found at such depth results in 
 [from] the watersheds [water-channels] having altered their courses, and carrying the 
 bones with the other drift, and fillmg up and levelling some large waterhole; the bones, 
 from their size and lightness, being the first deposited.” 
 
 * Eleventh Tri-monthly Report upon the Geological and Mineralogical Structure of New South Wales, 
 Sydney : Legislative Council Papers : 1858. 
 + Twelfth Tri-monthly Report, &c. Sydney: Legislative Council Papers: 1854, 
 
606 
 
 In 1869 the late Rev. W. B. Clarke reported * the discovery of a femur of a 
 Struthious Bird, subsequently named by Owen Dromornis australis, at the depth of 
 188 feet in drift resting on granite, from a well in that part of Peak Downs which 
 lies between Lord’s Table Mountain and the head of Theresa Creek, near the track 
 from Clermont to Broad Sound. The bone was found in a deposit of drift pebbles and 
 boulders one hundred and fifty feet thick, overlaid by thirty feet of black trappean 
 alluvial soil. 
 
 In the same communication, Mr. Clarke says, “In some of the creeks running more 
 to the south-eastward from the Peak Downs, and, like Theresa Creek, belonging to the 
 McKenzie River system (e.g., Crinum Creek), occur bones of Zrionyx and Crocodile.” 
 
 The late Mr. R. Daintree, in his Paper on the Geology of Queensland,t says :— 
 
 “From the Gulf of Carpentaria, in the north, to Darling Downs, in the south, 
 the fossil remains of extinct mammalia have been found in breccias and indurated 
 muds, which are representatives of the beds of old watercourses, through which the 
 present creeks cut their channels. At Maryvale Creek, in Latitude 19° 30’ South, good 
 sections of these old brecciated alluvia occur. The fossils from this section, as determined 
 by Professor Owen, are:—Diprotodon australis, Macropus Titan, Thylacoleo, Phascolomys, 
 Nototherium, Crocodile teeth, &c.t 
 
 ‘““Tmbedded in the same matrix occur several genera of mollusca of species 
 undistinguishable from those inhabiting the Maryvale Creek. My friend and late 
 colleague, Mr. Robert Etheridge, jun., has compared these with the Recent forms, and 
 finds them to consist of — 
 
 “ GasTEROPODA—Melania pagoda, M. arca, M. subimbricata, M. mesta, M. sp., 
 Limnea rimosa, Physa truncata, P. sp.§ 
 
 “ LAMELLIBRANCHIATA.—Corbicula australis; Unio, sp. 
 
 “The fact of these older alluvia forming both the bed and banks of the present 
 watercourse . . . . goes to prove that Diprotodon and its allies inhabited the 
 Queensland valleys when they presented little difference in physical aspect or elevation 
 from that of the present time. The Crocodile (Crocodilus australis), however, had then 
 a greater range inland than it has now. 
 
 ‘A study of these Diprotodon-breccias leads to the conclusion that the remains 
 were chiefly entombed in what were the most permanent ‘ waterholes’ in seasons of 
 excessive drought, and that the animals came there in a weak and exhausted state to 
 drink and die, just as bullocks do under similar conditions at the present time. 
 
 ‘“‘ No human bones, flint-flakes, or any kind of native weapon have yet been dis- 
 covered with the extinct mammalia of Queensland.” 
 
 In his Report “On the Geological Features of the South-eastern District of 
 Queensland,” || Mr. A. C. Gregory gives the following description of the “Older Alluvial 
 or Fossil Drift ”’:— 
 
 ‘The deposit is restricted to the valleys descending westerly from the main range 
 dividing the waters flowing to the east coast from those which flow westerly to the 
 Darling and Murray Rivers. Its limits are not well defined ; but it forms the banks of 
 the present watercourses, near the summit of the range, and extends down them to the 
 
 * Geological Magazine (1869), iv., p. 383. 
 
 t+ Quart. Journ. Geol. Soc. 1872, xxviii., p. 274. 
 
 {List corrected by my Colleague (sce Post-Tertiary Organic Remains) as follows :—Crocodilus 
 porosus ; Diprotodon australis, Owen; Macropus Titan, Owen. 
 
 § List corrected by my Colleague (Zbid.) as follows :—Corbicula nepeanensis, Lesson, Melania onca, 
 Adams and Angas, M. balonensis, Conrad, M. denisoniensis, Brot., Limnea vinosa, Adams and Angas, 
 Physa truncata, H. Adams. ‘ 
 
 || Brisbane : by Authority ; 1879, 
 
607 
 
 level plains near the banks of the Condamine River, where it appears to attain a depth 
 of more than a hundred feet, as fragments of bones have been obtained at that depth 
 in sinking wells. 
 
 ‘Tt may, however, be observed that, though the fossil drift is only found on the 
 - western waters in Southern Queensland, there are rich deposits in bone drift on eastern 
 waters of Peak Downs in the central district. 
 
 “This alluvium is remarkably rich in fragments of bones of extinct animals, 
 including Diprotodon australis, Macropus Titan, Thylacoleo, Phascolomys, Notothe- 
 rium, &e. 
 
 “The bones are associated with fragments of shells of Unio and other fresh-water 
 mollusea similar to those now found in the present watercourses, but more massive in 
 structure, basaltic pebbles, sand and mud, the stratification of which indicates inter- 
 mittent currents flowing down the present valleys, such as now result from the annual 
 rainfall, but of much greater volume. 
 
 “ Although the greater part of the bones are broken into fragments, and show 
 evidence of being drifted and waterworn, there are some which prove that many animals 
 cannot have been deposited before decomposition in the localities where their remains 
 are now found grouped together. 
 
 “The general condition under which the bones are found indicates that what are 
 now broad valleys and plains were originally extensive marshes with watercourses 
 flowing westward into lakes, and that the gradual filling up of the lake-beds with drift, 
 and the deepening of the channel of the Condamine River which drains the country, 
 conjoined probably with a gradual decrease in the annual rainfall, have combined to 
 change a swampy country covered with coarse, weedy vegetation into open downs and 
 plains producing short grasses totally inadequate for the support of animals with the 
 heavy frames and peculiar teeth which characterised the majority of the ancient 
 occupants of the district. 
 
 “There is no trace, either in the Darling Downs or any other part of Queensland, 
 of any violent convulsion of nature which would be adequate to cause the total 
 destruction of the Diprotodon and co-occupants of the country, and it seems most 
 probable that their extinction resulted from a gradual change of climate and more 
 effectual drainage through the deepening of the channels of the watercourses—aided, 
 perhaps, by some slight changes of level. Few satisfactory traces have been found of 
 the vegetation of this period, though some fragments of what appear to have been 
 woody seed-vessels are met with in the bone drift, but their condition is not sufficiently 
 perfect to admit of any definite conclusions. The general character of the vegetation 
 may, however, be surmised from the form of the animals, the structure of their teeth, 
 and the mode in which they are worn by feeding on it. These data suggest coarse reeds 
 and aquatic plants, such as would betoo succulent and liable to rapid decay for their 
 preservation as fossils, while the absence of wood and ferns, which are so abundant in 
 the older coal strata beneath, indicates that there was little or no forest. 
 
 “ One remarkable feature of the older alluvium is that the fossil bones are only 
 found in the detritus of the basaltic rocks. Alluvium of the same age, derived from the 
 Carbonaceous and Devonian Series, have not as yet been found to contain remains of the 
 extinct animals. This may have resulted from the superior fertility of the basaltic 
 lands, which would be capable of producing abundance of food, while the comparatively 
 sterile soil derived from the older formations would not furnish suitable vegetation for 
 the sustenance of the massive quadrupeds of that era.” 
 
 The occurrence of Diprotodon in the auriferous drift of Gogango Creek, near 
 Rockhampton, is noted by Mr. Daintree in his “General Report on the Northern 
 
608 
 
 District.” * This specimen was said to be in the possession of Mr. John Jardime, Gold 
 Commissioner (now deccased), Gogango, according to the Railway Survey, is only 
 three hundred and fifteen feet above sea-level. 
 
 A. portion of a lower jaw of a Diprotodon, pronounced by Dr. EH. P. Ramsay, 
 Curator of the Australian Museum, Sydney, to be probably the young of D. 
 australis, or perhaps a new species, was found by Mr. T. Buckland on the bank of | 
 the Burdekin, opposite Gilgunyah Station. A cast is in the Geological Survey 
 Museum. 
 
 Taking the Maryvale, Burdekin, Peak Downs, and Darling Downs localities, from 
 which remains of the extinct mammalia have been obtained, it will be seen that all these 
 places are at considerable elevations, none of them being less than 900 feet above 
 the sea-level. Caiwaroo, where Mr. Cotter’s fossils have been obtained, must be about 
 400 feet above the sea. The doubtful instance of Gogango Creek would, however, 
 bring the fossils down to 315 feet. The only instance of which I am aware of remains 
 of the extinct mammalia having been obtained near the sea-level is that of the Hight- 
 mile Plains, near Brisbane. ; 
 
 There is abundant evidence + to show that in the southern Colonies the extinct 
 mammalia existed in Pliocene times. On the other hand, in Queensland there is no 
 evidence that they went back to the Tertiary Epoch, although it is quite possible that 
 they did. Such direct evidence as we have, consisting of the association of the mammalia 
 with fresh-water and land shells of species still living, would lead to the conclusion that 
 the former were, in the Queensland area, confined to the Post-Tertiary deposits. Still, 
 considering how imperfect is our knowledge of the Tertiary in Queensland, we may 
 well be prepared for the production of fresh evidence on this point. 
 
 The introduction of the peculiar Mammalian and Avian Tertiary and Post-Tertiary 
 Fauna into Australia is one of the most puzzling problems offered by geological history. 
 Mr. Alfred Russell Wallace says :— 
 
 ‘Marsupials are almost certainly a recent introduction into South and North 
 America from Asia. They existed in Europe in Eocene and Miocene times, and 
 presumably over a considerable part of the Old World; but no trace of them appears in 
 North or South America before the Post-Pliocene period.’ 
 
 It must not be understood that the first appearance of marsupials in Europe was 
 in Eocene times, as they are known as far back as Triassic. The migration of marsupials 
 from Europe and Asia to America may have been accompanied or preceded by a migration 
 from Asia to Australia by way of a land connection formerly existing. At any rate, 
 marsupials make their first appearance in Australia in Pliocene times, and in great force. 
 There is no paleontological warrant for the supposition that they originated in Australia , 
 The migration of marsupials does not appear to have extended to New Zealand, although 
 a land connection seems to have existed in Cretaceous times, but not later.§ The 
 wingless birds of New Zealand and Australia, both fossil and recent, present evidences of 
 former connection ; but as their avian ancestors may have possessed the power of flight 
 and even of swimming,|| their distribution may have been more rapid than that of the 
 mammalia, and may have extended to New Zealand before the land connection was cut 
 
 * Page 4. Brisbane: by Authority: 1870. 
 
 + Notes on the Geology of New South Wales, by C. S. Wilkinson, p. 57. Sydney: by Authority : 
 1882. 
 
 + Geographical Distribution of Animals, i., p. 155. London, 1876. 
 
 § Professor Hutton. ‘‘ On the Origin of the Fauna and Flora of New Zealand.” Presidential Address 
 to the Philosophical Institute of Canterbury, 1st November, 1883, Pt. i., p. 17. 
 
 || See A. R. Wallace, p. 451. Island Life. London, 1880, 
 
 
 
609 
 
 off. The generic and specific distinctions between the marsupials and the wingless birds of 
 
 ethe Old and New Worlds and of Australia and New Zealand may have arisen during 
 the progress of migration, and may have been further developed by the insulation which 
 Australia and New Zealand subsequently attained. 
 
 The extinction of the same fauna, which had a, geologically speaking, brief 
 existence in Australia, has been accounted for by Professor Owen and Professor Tate 
 by the intervention of Man; and by the late Mr. C. S. Wilkinson by the supervention of 
 the present arid climate on a period of heavy rainfall, which there is evidence to show 
 occurred, after Pliocene times.* Mr. Wilkinson argued that heavy rainfall and con- 
 sequent luxuriance of vegetation were necessary for the support of the numerous and 
 in some cases gigantic animals of which we have now only the fossil bones. Darwin 
 has, however, shown f in the most striking manner that the regions which in the present 
 day support the largest and most numerous quadrupeds are by no means those which 
 are most remarkable for luxuriance of vegetation ; nor, conversely, are the regions now 
 most characterised by luxuriance of vegetation the favourite haunts of large animals. 
 As for the intervention of Man, it will be seen in a succeeding page that the evidence 
 in favour of his existence in Australia coeval with the extinct Post-Tertiary Fauna is at 
 least doubtful. 
 
 I do not mean to advance a thesis which I am prepared to defend against 
 all comers, when I suggest that the extinction of the Post-Tertiary Mammalia, &c., may 
 have had something to do with the subsidence afterwards referred to,f but simply draw 
 attention to a factor which appears to have been overlooked. It is not unreasonable 
 to suppose that changes of climate followed, on the subsidence of the land, sufficiently 
 great to have a disastrous effect on the now extinct fauna. It is also possible that 
 when the shores of the Great Australian Bight were ground down by ice, the climate 
 may have been too rigorous for their existence even on the Darling Downs and the 
 tropical portions of Queensland. 
 
 CAVES. 
 
 None of the Caves which penetrate the limestones of Queensland have yet been 
 systematically explored. They may yet prove as interesting for their imbedded organic 
 remains as the Wellington Cave itself. Some of these caves may be here described :— 
 
 The limestones of the Chillagoe District (Gympie Beds ?) are remarkable for the 
 number and size of the caverns which have been excavated. I was informed by Mr. 
 H. G. Livesey, of Irvinebank, who has made numerous admirable photographs of the 
 scenery of this remarkable region, that at least thirty caves are already known. I 
 visited, under the guidance of Mr. W. Atherton, of Chillagoe Station, the cave known 
 as “The Temple,” which occurs in one of the limestone ranges on the left bank of 
 Chillagoe Creek, about two miles from the Station. Entering by a lofty opening on the 
 western side of the range, we walked erect for perhaps sixty yards, and then found 
 ourselves in a magnificent theatre, about one hundred feet in diameter and some eighty 
 feet high. The cupola-like interior was lighted from the top by a hole which had an 
 area of perhaps two hundred square feet. The roof was festooned with stalactites, while 
 the floor was covered in places with stalagmite. Occasionally these met, forming 
 long and graceful columns. But the stalactites and stalagmites were rarer than is 
 
 * Anniversary Address to the Royal Society of New South Wales, 2nd May, 1888. 
 + Journal, Voyage of H.M.S. ‘‘Beagle” Round the World ; Chap. v. 
 + Sce remarks on the depths of the drifts in the neighbourhood of Townsville. 
 
 2P 
 
610 
 
 usually the case in limestone caves, this circumstance probably pointing'to the dryness 
 of the climate. The greater part of the floor was deeply covered with drab-coloured 
 “cave-earth,’ vepresenting probably the insoluble argillaceous impurities of the 
 limestone. Shells of Helix, in all stages of incrustation by lime, were plentifully 
 scattered over the floor in some places—probably the sites of pools in wet weather. 
 On one side of the “‘theatre” a dark recess opened out, its lower half blocked by a nearly 
 flat limestone boulder, in front of which a row of stalactites depended from the roof 
 like a partially uplifted curtain. Perhaps the most picturesque aspect of the cave was 
 that seen from behind the stage, looking past this screen into the proscenium. A 
 narrow passage behind the stage led to other caves, some at lower and some at higher 
 levels. One of these must have been at least two hundred feet in length, and 
 fifty feet in width, with a gothic roof eighty feet high. There were many nooks 
 where the stalactites were little thicker than pencils, and arranged in groups of 
 exquisite beauty. Very few of them had, at the date of our visit, the drop of water 
 which one expects to find in such a position. From a few, drops of water fell at 
 very long intervals. The floors of the caves appeared to be about on a level with the 
 surrounding country, and, according to Mr. Livesey, this is usually the case with the 
 caves of the district.* 
 
 The Middle Devonian Limestone of the Broken River, a tributary of the Clarke, 
 contains numerous caves, from the detritus on ‘the floors of which gold is said to have 
 been obtained. 
 
 The limestone beds of the same-age near the Fanning Station also contain 
 beautiful if not large caverns, adorned with stalactites. 
 
 The caves in the limestones of Raglan and Langmorn, Port Curtis, have been 
 described by the late Mr. James Smith} as large and picturesque. Mr. Smith has 
 obtained from the stalagmitic deposit on the floors some fragments of bones, still 
 undetermined, together with recent land shells, and has also noted the occurrence 
 of a deposit of stalagmite, containing fossil bones, from which the limestone that 
 formerly enclosed them has been entirely weathered away. 
 
 In the neighbourhood of Rockhampton numerous caves occur in the immensely 
 thick limestone beds of the Gympie Series. Some of these were explored to some 
 extent by Mr. Smith, whose descriptions (somewhat condensed) are quoted below. 
 Making every allowance for Mr. Smith’s well-known enthusiasm, it is evident that 
 the caves are worthy of systematic and scientific investigation.t It may be added 
 that Mr. Smith’s determination of species may be incorrect, and in point of fact my 
 Colleazue does not adopt them, as further collections will be made. 
 
 Olsen’s Caves.—* Traversing these long, extensive subterranean passages, lofty 
 galleries, spacious chambers, and wide spanning arches, by the light of a candle that but 
 reveals the gloom, you cannot help becoming possessed with a sense of solemnity and awe 
 in the presence of Nature’s mysteries. But these walls are not of a black and ghastly 
 funereal hue. They are everywhere of a neutral tint of shaded white, abundantly 
 tapestried with encrusting infloresence, panelled with curiously-carved pendentand planted 
 alabaster decorations, and clothed with many hangings of petrified cascades, entirely 
 made up of minute hexagonal, needle-pointed, reversed crystals of purest calcite. Do 
 these caves contain any records throwing any light on the conditions of local former life ? 
 This is a problem that will provide occupation for many labourers for long years to 
 come. 
 
 
 
 * Report by R.L.J. on the Chillagoe and Kooboora Mining Districts. Brisbane: by Authority : 1891. 
 t+ MS. notes. 
 + Mr. W. H. Rands has recently examined the Caves, and his Report will shortly be published. 
 
611 
 
 “What has been done already is interesting enough, but nothing very strange, 
 wonderful, or startlingly new as yet. The shells and bones locked in the stalagma and 
 those found loose in the bat exuvie are identical with those of existing species. Casts 
 of fossil millipedes are among them. 
 
 “The first new cave is in a low mound, a few hundred yards to the left of the 
 big hill. You descend a deep, narrow shaft by méans of a rope half-way, and there is 
 a further descent by leaping from one projection to another, in a slanting direction, till 
 you come to the bone-bed. There is no foul air; ventilation seems to come from 
 another opening, but there is the closeness of the charnel-house, and the mustiness 
 of the tomb. The bones-are the remains of a large Kangaroo. The leg bones are 
 sixteen inches, and thigh bone ten inches. The lower jaw was originally ten inches long. 
 I did not see the skuil. They are very decomposed and crumbly. I think the Raita 
 must have fallen down the shaft, and floundered along in its uninjured state to the 
 centre of the deep cave where it was lying. In the other new caves adjoining, a com- 
 plete skull of a Native Cat, with its retractile teeth, and several Wallaby and Opossum 
 skulls, with other remains, were found. These bones are now on view at the School of 
 Arts, Rockhampton. 
 
 “The beauty, cleanness, variety, and number of the ornaments in these new 
 vaults far exceed anything to be found in the larger caverns. These are the realisation 
 of the works of the most wonderful genii of our youth, the elaborate grottos of the 
 fairy tales. Ladders are to be placed. so that they may be reached, and, above every- 
 thing, they ought to be wire-netted. 
 
 “The increasing value of what was once termed ‘ the waste lands of Australia’ 
 suggests attention to her waste products. Contemplation of the vast mounds and deep 
 deposits of the bat manure, mixed with the pulverulent lime marl in these caves, points 
 to large sums of money that may be realised from their utilisation. From what I have 
 read of what is being done with this substance in other places, its value is sufficiently 
 established.’’* 
 
 Johannsen’s Caves.—‘‘ These caves are situated contiguous to our local ‘ Mount 
 Etna.’ They are in a great mountain of compact limestone—a grey, dense marble, 
 exactly corresponding to the rock of Gibraltar, hard, homogeneous, and unstratified, 
 but cracked and tilted in thick irregular beds. The outside weathering is of the usual 
 sharp-pointed, pock-pitted nature all these formations throughout the district present to 
 the eye. All round the base of the mountain are the usual fallen masses, and the 
 numerous lumps of thin stratified stalagma among them tell how cave action has reduced 
 the hill to half its former size. The chief entrance is greatly blocked up by the fallen 
 roof of a former cave. One feature of Johannsen’s Caves is their narrow entrances, 
 and their wide swelling proportions inside. You crawl and creep through a ‘hole in the 
 ground’ that hardly admits you, and in a moment you may walk for six solid hours 
 through the great squares, wide streets, intricate labyrinthian mazes, circling wynds, 
 courtyards, and lanes, ‘through-gaun closes’ of a great subterranean town with 
 surrounding suburbs. The architecture is entirely gothic, of cathedral form; and the 
 strong impression besets you that you have stumbled on the ruins of a medieval 
 city. The black gloom of these lofty corridors, of which no candle can show the roof, 
 and the great groined arcades, with rear aisles, deep secret recess-arched alcoves, 
 and hanging rock-flitches, must be seen to be appreciated. They beggar description. 
 
 “One of the beaiaeieal points is a black bed-crack circling round all the central 
 caves, about the height of a man’s head, showing that in former times the whole 
 
 * Rockhampton Bulletin, 12th October, 1886. Mr. Rands, whoj has since visited the caves, does not 
 think that the bat manure can be profitably worked. 
 
612 
 
 formation was connected together like solid steel, and that the whole thing has been 
 slowly cut out of the cracks and crevices by the agency of water percolation, holding a 
 modicum of carbonic acid in solution. 
 
 “The tale of the economic value contained in these caves may well come in here. 
 Capitalists, sighing for profitable investments, sink to the knees at every step in the 
 most fructifying of all materials, consisting of deep deposits of bat exuvie that must 
 have taken millions of years to accumulate, mixed with a floeculent lime powder that 
 slowly drops from the rock faces, and is the undoubted agency that has melted them 
 away. If allthis be true of mere naked nothingness, enormous vacuity, black and 
 murky midnight darkness, what shall be said when you begin to see these walls clothed 
 in snowy whiteness, the niches filled with the nicest carved statuettes, the arched 
 alcoves framed in the most unique of alabaster pilasters, the floors studded with the 
 rarest forms of marble columns, the roofs an inverted forest of pendent cones, and the 
 tout ensemble a glittering mass of saccharine, granular, glancing, acicular crystals, 
 beyond the power of pencil to paint, designer to plan, or heart to conceive. 
 
 “Our party was the first of the public to conquer the ‘deep sink.’ Progression 
 was like gasteropods, and, feet foremost, through the narrow tunnel, deep down a series 
 of perpendicular ladder-flights, lashed together with iron wire. At the bottom of this 
 series of caves there isa burst of exclamation of mingled astonishment, rapture, and 
 delight. The wide floor is covered with shells, like a sea shore, crunch-crunching at 
 every step. But the chief feature is a perennial bubbling fountain, like a cold-water 
 geyser, that has built a wide mound, in a succession of tiny terraces. The structure of 
 these overflowing circles is of the cellular rhomboid form of the inside coating of a 
 bullock’s stomach, and has been named ‘tripe-stone.’ From numerous dried-up 
 formations of this shape, throughout all the caves, we have the evidence of very much 
 of this work having been done in the past. It is a petrifying spring. The water is as 
 clear as glass, as cold as ice, tasteless, and palatable. This is where the fossils are 
 found ; and the samples show every stage of the process—the bright bands of the 
 scrolled shells beginning to be coated, others deeply incrusted, and some turned to balls 
 of solid marble. The teeth in the skulls and the incrusted shank bones are very 
 remarkable and deeply interesting, for these are the things that Science asks for, and 
 care will be taken that they will be placed in proper hands. Any object you desire to 
 be turned into stone, from a human being to a spider’s web, has simply to be immersed 
 for a time on the shelves of these terraces, in that lime-water. 
 
 “But Nature has built the most handsome of all her ornaments, the chastest, 
 most delicate, superb, and beautiful of these cave treasures away up in the most secret 
 recess of the ‘ benmast bore.’ 
 
 ‘“‘As high up again as you have descended, overhead high benches and long, sloping 
 moraines—in an upper corner a great cluster of twin wavy, stalasso, in projected 
 canopy, semi-circular form, joined to the wall with the widest, deepest, folded curtain 
 drapery of the most curious dendritic weaving that ever eyes saw. 
 
 “We visited the Crystal Cave, replete with the most magnificent slabs of com- 
 pressed, pure calcite crystals.” 
 
 Mr. Smith sent mea small collection (now in the Geological Survey Museum) of 
 bones dug by him from the stalagmitic floor of Johannsen’s Cave, together with the 
 following notes by Mr. C. W. De Vis, dated 1887 :— 
 
 Nos. 
 
 184. Chip from inner fore side of right radius of Horse. 
 
 185. Right femur of young Kangaroo Rat (Hypsiprimnus sp.). Uniess the Rockhampton species 
 differs much from the common H., rufescens and H. Greyi, this bone is significant. 
 
613 
 Nos. 
 186. Right side of pelvis, hardly distinguishable from that of Malmaturus temporalis, the 
 Moreton Bay “ Padymelon.”’ 
 
 187 and. 196. Right mandibular ramus of Phalangista canina (Opossum). [No. 187 sent to 
 Queensland Museum. ] 
 
 188 and 191. Left tibia of a “Padymelon.’ Unlike any existing species available for 
 comparison. 
 
 189. Left side of pelvis of Rock Waliaby. Possibly Petrogale penicillata. 
 
 190. Part of left mandibular ramus of a little Wallaby, smaller than any living species known 
 tome. [Sent to Queensland Museum. ] 
 
 192. Small bone, too delicate for manipulation. 
 
 193. Apparently the outer metatarsal of a Kangaroo Rat. (Compare 185.) 
 
 194. Part of skull of young “ Padymelon.” The nearest living species is Halmaturus stigmaticus, 
 of the Cairns district. 
 
 195. Femur of young Kangaroo Rat, of larger size specifically (?) than No. 185. 
 
 197. Upper canine of a large Opossum, Phalangista, sp. 
 
 198. Right mandibular ramus of a Bandicoot. Very like, if not identical with, Perameles 
 nasuta. 
 
 199. Second upper molar, off side of a Horse.* 
 
 It may be remarked that my Colleague has determined four species of Helix, all 
 living in the district, as occurring with the bones in the stalaymite deposit of Olsen’s 
 and Johannsen’s Caves. The constant association of Recent land and freshwater 
 mollusca with the remains of the extinct mammalia and birds in the drift beds has 
 already been noticed. 
 
 From Cape Palmerston to the mouth of the Herbert River, the eastern coast is 
 fringed by a strip of alluvial flat, varying in breadth up to thirty miles or more. 
 Although apparently level to the eye, it attains an elevation of nearly three hundred 
 feet at the base of the Coast Range west of Townsville. Whether seen on the spot, or 
 as delineated on the Geological Map, the first idea of the observer is naturally that this 
 alluvial flat is a Raised Beach; but, in spite of the presence of beds of clay well fitted to 
 preserve fossils, no remains of marine organisms have ever, so far as I have been able to 
 learn, been discovered in it. 
 
 Numerous bores and wells have proved this flat to be composed of alternating 
 beds of clay, sands, and gravels, the latter being sometimes cemented or consolidated. The 
 gravel, which is sometimes very coarse, contains well-rounded pebbles or boulders such 
 as probably belonged to river beds. In the neighbourhood of Townsville, a bore (Bore 4) 
 at the Hubert Well did not “‘ bottom” these drifts at 125 feet; a bore (Twaddle’s No. 2) 
 in Portion 100 (Stewart's Creek) had 101 feet of drift; and another in the same Portion 
 (Twaddle’s No. 4) had 109 feet of drift. As the sites of these bores are not more than 
 thirty feet above the sea, the “ rock-head,” or old land surface, must be from eighty to one 
 hundred feet below the present sea-level. No river could possibly have excavated a 
 channel to this depth while the land stood at its present level. The land, therefore, must 
 have been depressed to or beyond the position at which it now stands with reference to 
 the ocean. Moreover, if, as I believe, the alluvia referred to are those of land valleys 
 (lakes or rivers), their western walls or rim-rocks must have occupied sites now marked 
 by islands in the Pacific or submerged or carried away by marine erosion. Fragments 
 of this lost land remain, I believe, in Fitzroy Island, Hinchinbrook Island, the Palm 
 Isles, Magnetic Island, Cape Cleveland, Feltham Cone, Cape Upstart, Gloucester 
 Island, and the Whitsunday, Cumberland, Beverley, and Percy Islands; while a 
 submerged range still further to the east may be represented by the Barrier Reef. 
 
 
 
 
 
 
 
 * The occurrence of the remains of the Horse quite destroys the interest which would otherwise attach 
 itself to this deposit from a geological point of view. (R.Z. Junr.) | 
 
614 
 
 This submergence, in all probability, took place after the period to which the 
 Extinct Mammalia belonged. It is probably the same submergence to which the late 
 Rey. J. E. Tenison Woods attributed * the formation of Sydney Harbour. I am quite 
 in accord with Mr. Woods on this point, as the harbour has all the appearance of a 
 submerged land valley, 
 
 The late Mr. C. 8S. Wilkinson ascribed + the depression which created Sydney 
 Harbour to certain faults which divide the tableland of the Blue Mountains from the 
 low-lying coast country, arguing that the faulting took place towards the close of the 
 Tertiary Epoch, “for no marine Tertiary deposits are known along this portion of the 
 coast of Australia, whereas in New Guinea on the north, and in Victoria on the south, 
 the marine Mivcene beds occur at elevations up to eight hundred feet above the sea. 
 Had this low-lying country along the East coast of Australia then existed, it must have 
 been covered by the Miocene sea, and doubtless some traces of the marine strata of that 
 period would have eseaped denudation and remained, as those have which are seen in 
 Victoria and elsewhere; but it is very probable that until or during the Pliocene period 
 it stood above the sea-level and extended some distance beyond the present coast line. 
 Then, again, the Tertiary deposits throughout East Australia show that the valleys 
 draining the Great Dividing Range have been chiefly eroded since the Miocene period, 
 for we find deep valleys and ravines cutting through later Tertiary formations; there- 
 fore the sinking of the land traversed by any of these valleys—such as that of Port 
 Jackson—evidently took place in comparatively receut geological times, and may have 
 been contemporaneous with the extensive volcanic eruptions of the Upper Pliocene 
 period during which the southern portion of Victoria especially was the locale of great 
 voleanic activity.” 
 
 I regret that I cannot agree with the reasoning of my lamented friend, so far as 
 regards the age of the faults in question. All that is certain on this point is that the 
 faulting took place at a period subsequent to the deposition of the strata which they 
 disturb, as no strata of later date are superimposed on the faults themselves. There is 
 no evidence that a low-lying country was immediately produced on the down-throw sides 
 of the faults. The country east of the faults may have remained during Miocene times 
 at a level high enough to be above the reach of the Miocene sea, and may have only 
 
 since then been reduced by sub-aérial denudation to the present level. The argument — 
 
 from “deep valleys and ravines cutting through later Tertiary formations ”’ fixes the 
 oldest possible, but by no means the newest possible date for the depression of the land 
 surface resulting in the formation of Port Jackson. 
 
 It need excite no surprise that the same Geologist who denied that the Desert 
 Sandstone had been laid down at a lower level than that at which it is now found refused 
 to admit that ‘ one well-reeorded observation has been brought forward” in proof of 
 recent elevation on the Eastern coast.{ Nevertheless, there are several observations on 
 this point which must be treated with respect. 
 
 Near Cape York, Dr. Alexr. Rattray, Surgeon, R.N., noted§ several circumstances 
 which prove that Raine Island has in Recent and even in modern times risen from its 
 former position. He says:— 
 
 “Raine Island, which possesses its own special and active fringing reef, is low, flat, 
 about one-third of a mile long, and a quarter of amile broad. Itrises about ten feet above 
 
 * Journ. R. Soc. N. S. Wales, 1882-1883, xvi., p. 58. The Hawkesbury Sandstone. 
 
 + Notes on the Geology of New South Wales. 2nd. Edition, p. 70. Sydney: by Authority : 1887. . 
 
 t Rev. J. E. Tenison Woods. Geology of Northern Queensland. TZrans. Queensland Philosophical 
 Society, 20th December, 1880. 
 
 § Notes on the Geology of Cape York Peninsula. Quart. Juwrn. Geol. Soc., xxv. (1869), p. 303. 
 
 
 
 | 
 
615 y 
 
 high water, and consists of hard, compact, brecciated coral conglomerate, with a shelving 
 beach of coarse coralline and shelly sand, anda scanty superstratum composed of the coral 
 débris sparingly mixed with vegetable matter, and a thin layer of guano deposited by the 
 numerous turtle and flocks of terns, gannets, and other aquatic birds that, like the former, 
 make this their headquarters and favourite breeding-place. The whole constitutes a soil 
 capable of supporting a scanty vegetation of weeds, coarse grass, and creepers, but some- 
 times—as at Cairncross, the Howicks, Pipers, and many others— a dense scrub and well- 
 grown mangroves—Casuarine, Pandani, Pasonie—and other trees common along this 
 coast. Of this organic rock the beacon on Raine Island was built eighteen or nineteen 
 years ago ; and the durability of the material is shown by the fact that the structure has 
 hitherto undergone no decay from weathering.. It doubtless tops some crystalline 
 formation, on which it has been slowly reared. Still, it is evident that, though now 
 permanently out of, it must have been formed while under water, and have reached the 
 surface at low water with the zoophytes which built it in full activity, when the greater 
 part of the long reef now in full activity at the sea-level at ebb, and of which it forms 
 only a fractitional part, was still many feet below. And now, when the latter has 
 reached close to the surface at low water, the former projects twenty feet in the air, 
 but denuded by weathering of its soft and brittle exterior, with its dense solid interior 
 laid bare, and its living, many-hued, branching madrepores repiaoee by less gaudy forms 
 of vegetable life. 
 
 “‘ Between the active coral reef still under water and the extinct ones now well 
 raised above it, like Raine Island, we meet with many intermediate forms, occasionally 
 as islets which consist of a sand-bank just showing above the surface, and either still 
 unclad with vegetation or having a few sprouts of mangrove, the hardiest of trees, and 
 usually the first to find a ene in the coarse coral debris , little capable, to all appear- 
 ances, of sustaining life of any sort, while others show rte elevation, and both more 
 extensive and better-clad area. In short, we find islands of this class in many different 
 stages of upward progress, sometimes forming part of the reef, but more usually lying 
 between it and the mainland.”’ 
 
 The late Professer J. B. Jukes mentioned* the occurrence of pumice pebbles on 
 a plain on the west side of Lizard Island, “at least one or two hundred yards back from 
 the sea, and several feet above any possible tide.” 
 
 A. Raised Beach extends for five miles north of Camisade Creek, Temple Bay. 
 It is ten or twelve feet above high-water mirk, is nearly a quarter of a mile in breadth, 
 and is covered in places with blown sand. I have reason to remember this locality, 
 where I was speared through the neck in the course of a murderous attack by the 
 blacks, who filled up the tents of the party with spears. 
 
 Mr. G. Elphinstone Dalrymple, in his Narrative of the Queensland North-east 
 Coast Expedition, 1873, (p. 16,)¢ refers to a “high beach of broken coral, shells, and 
 granite detritus,” on the north-west side of Fitzroy Island, and adds:—‘“ Here there is 
 a recurrence of the old raised beaches and pumice pebbles rising in successive steps from 
 the sea-level.” 
 
 Mr. W. Saville Kent, I'.L.S., in a Presidential Address to the Royal Society of 
 Queensland (22nd November, 1890),§ has the following :— 
 
 ‘“‘ Apart from the vital processes by which reefs and their component corals are 
 continually adding to their bulk, there can be but little doubt that a slow motion of 
 
 * Narrative of the Surveying Voyage of H.M.S. ‘‘Fly,” i, p. 95. London, 1847. 
 +Report by R.L.J. on Explorations in Cape York Peninsula, 1879-80. Brisbane: by Authority ; 
 1881, p. 41. 
 
 { Brisbane: by Authority: 1874. 
 § Proc. Ann. Meeting Roy. Soc. Queensland. Brisbane, 1891, p. 38. 
 
 
 
 
 
616 
 
 upheaval is progressing throughout the region of Torres Straits and the Great Barrier 
 system, and this, too, must tend towards rendering the older charts untrustworthy. 
 The coral reefs volunteer their own evidence upon this point. At many stations 
 throughout this region the-cireumstances may be noted that large expanses of dead coral 
 intervene between high water mark and the living banks. This dead coral here referred 
 to, is not the broken débris that has been cast up by storms, such as commonly exists 
 all along extreme high water mark; but occurs at a lower level 2m situ as it originally 
 grew, and is only lacking in vitality to distinguish it from the living reefs. The Albany 
 pass between Cape York and Albany Island, yields a prominent illustration of this 
 phenomenon. On either side of the passage there isa fringing coral reef, the living 
 inner margin of which, composed chiefly of a branching Madrepore, is only exposed at 
 the lowest spring tides. Immediately adjoining this living bank, between it and the 
 foreshore, there is a belt of the same species of coral, but entirely dead and brittle, 
 like rotten ice to walk upon. Within a few more years this dead belt will no doubt 
 be. broken up by the action of the waves and chemical disintegration, and be 
 added to the existing inshore area of coral mud and débris. An examination 
 of “the circumstances that have brought about the present condition of the 
 reef shows that this dead belt of coral is now exposed to atmospheric 
 influences, which are antagonistic to its growth, with every ordinary spring tide; 
 while the living coral, as’ before observed, is only visible above the water at the 
 exceptional or lowest springs. At the period that the inner belt of dead madrepora 
 was alive, and which from its state of preservation cannot be long ago, it must have 
 grown at a similar lower level as that now living, and nothing but the general upheaval 
 of the area on which it throve can logically explain the fact of its decadence. The 
 fringing reef off Magnetic Island, near Townsville, presents closely analogous 
 phenomena. Dead bivalve shells of large size, such as Tridacnas and Pinnas, also 
 occupy their original positions here, in close contiguity to the dead corals. Yet more 
 substantial evidence of the upheaval in this district was afforded me by a station-holder 
 on Magnetic Island, and by whom I was informed that within the time he had 
 been located there a very perceptible change had taken place in the small bay facing 
 his property. In former years boats could approach the landing-place at all tides, 
 excepting very low springs, whereas now it was not possible to bring a boat in at even 
 ordinary low tide. The shallowing of the water could not be accounted for by the 
 silting up of the bay, there being no fresh water flowing into it, while the rocky bed of 
 the bay itself had apparently been raised to a higher level. The instances now recorded 
 might easily be multiplied.” 
 
 Mr. Maitland describes * the occurrence of stranded pumice in various parts of 
 Magnetic Island, notably on those portions most exposed to the open sea, and adds that 
 he never observed it at a greater elevation than twelve feet above sea level. “ The rounded. 
 form and somewhat decayed interior presented by many of the pebbles, bear evidence 
 of their having travelled some considerable distance, and as has been noticed by various 
 observers in many islands of the Pacific, pieces were found incrusted with calcareous 
 tubes of the tubicular annelids, Serpula and Spirorbis. The source of these pumice 
 drifts is to be looked for in many of the volcanic islands with which the Pacific is known 
 to be studded.” 
 
 I am informed. by Mr. Joseph Hughes, Sub-collector of Customs, Townsville, that 
 on Rattlesnake Island a deposit of dead coral, similar to that described by Mr. Saville 
 Kent, occurs at about five feet above high water mark. 
 
 
 
 
 
 * Report on Magnetic Island? Brisbane: by Authority: 1892. 
 
 
 
617 
 
 In Ross Island, Townsville, near the mouth of the Ross River, a thick bed of clay 
 forms part of an estuarine deposit above high water mark. This is a “ Raised Beach,” in 
 the ordinary sense of the term. It is crowded with fossil shells, and the late Professor 
 Denton having insisted that it was of Tertiary age, I made a collection, which my Col- 
 league examined and found to consist entirely of species still living in the adjoining seas. 
 
 The late Prof. Jukes, speaking of the coast flats near Cape Upstart,* referred to 
 pebbles of pumice found among the grass and under the roots of the trees “ wherever 
 we landed, from Sandy Cape to this place,” and added, “ I have never observed them 
 at a greater height above the sea than fifteen feet.”” I can confirm Prof. Jukes’ remarks 
 and extend them to almost every part of the Eastern Coast I have visited. 
 
 Speaking of the coral conglomerate of Cape Upstart and the Capricorn Islands, 
 Prof. Jukes remarked + :— 
 
 “ Flats composed of it, half-a-mile in width, are frequent along the shore of the 
 north-east coast of Australia. Upon all these flat spaces formed of the conglomerate, as 
 well as upon all other flat land along the eastern and north-eastern coast of Australia, 
 which is not more than ten feet above high water mark, there is found an abundance of 
 pumice pebbles. They are never, or very rarely, seen on the present beach or recently 
 washed up, nor are they found now floating at sea. . . . They are also found 
 embedded in the coral rock of Raine’s Islet. Whatever age, therefore, may be given to 
 the coral conglomerates must be extended to the pebbles.” 
 
 In the neighbourhood of Nudgee, near the mouth of the Brisbane River, a sandy 
 Raised Beach, perhdps twenty feet above sea level, contains an abundance of fossil 
 shells all of living Pacific species—at least no other have been detected in a collection 
 made by me and critically examined by my Colleague. 
 
 Speaking of Peel Island, Moreton Bay, Mr. Stutchbury wrote t in 1854 :— 
 
 “Tn proof of its modern but gradual uprising, I offer the following facts:— 
 “The whole length of the beach on the eastern side, above the present water line, 
 is studded with dead coral in situ naturale, much of it never having been removed 
 from the place in which it lived, principally consisting of the genera Meandrina, 
 Astrea, and other shallow water corals. It is known that these genera, although 
 capable of living in very shallow water, cannot exist the length of an ebb tide unless 
 there is a spray sea wetting them, and, as it does occur that at occasional times, during 
 changes of wind or calm, they would be left perfectly dry for six or seven hours, then, from 
 the delicate nature of their structure they would be destroyed, and such is the case here 
 exhibited. In addition, I find that in the shallow waters—now mere sandbanks (which 
 may be waded at a depth of three or four feet) of areas of hundreds of acres—there may be 
 seen Pocillopora, Caryophyllee, and other genera which only exist in tolerably deep 
 water, z.¢., from five to ten fathoms. No living species of the latter genera are now to be 
 found in the bay. I endeavoured to obtain them by the dredge, but without success, but 
 on the shallow banks, always covered even at low-water, fine examples of the first-named 
 genera may still be found alive. Further, several feet above the present high-water line, 
 clumps of dead rock-oysters may still be seen adhering to the rocks on which they grew. 
 
 “The above facts, taken together with those seen in the islands of the River 
 Hunter, described in the Report of my trip to Newcastle and Maitland in December, 
 1850, I think are sufficient to prove that the whole of this vast island [Australia] is still 
 gradually emerging from the ocean.” 
 
 * Narrative of the Surveying Voyage of H.M.S, ‘‘ Fly,” i., p. 53. London, 1847. 
 + Loc. cit. p. 335. 
 
 { Twelfth Tri-monthly Report upon the Geological and Mineralogical Survey of New South Wales. 
 Legislative Assembly Paper, N.S. Wales, p. 7. 
 
618 
 
 In his next (Thirteenth) Report Mr. Stutchbury gave furtner proofs of the 
 modern uprising of the land in Moreton Bay District, under date 20th May, 1854 :— 
 
 “At Luggage Point* I found the remains of a skeleton of an exceeding large whale 
 which had been thrown whole upon the beach. It was much decomposed, every cell in 
 the bones being filled with mud, and deposited just within the verge of the present high 
 water mark, in fact in such a position that it would have been impossible for the highest 
 waves to have rolled it from deep water over the extensive shoals which lie out in this 
 direction.”’ 
 
 On Bribie Island “the whole of the eastern seaward coast is composed of the 
 purest sand, with scarcely a pebble intermixed—an east and west section showing, in a 
 line of a quarter of a mile in length, several distinct parallels of shore—a further 
 instance of the fact of upheaval.” 
 
 In his “ Sixteenth Report,’ dated 20th November, 1855, Mr. Stutchbury has the 
 following note on Fraser Island: — 
 
 “The curvilinear beach between South Trees Point and Barney Point presents 
 an immense barrier of marine shells, extending far above the present high tide limit, 
 and a few yards further inland considerable quantities of detrital pumice may be 
 observed. This occurrence of pumice above the tidal lines of this period presents itself 
 along the whole of the north-eastern shores, especially on the eastern or ocean beach of 
 the Great Sandy Island.” 
 
 Mr. Alexander Macpherson read a Paper before the Royal Society of Queensland, 
 on 7th August, 1890, showing from observations at Sandgate and Nudgee that the land 
 at the mouth of the Brisbane River is gradually being elevated. 
 
 As shown in an exhaustive Memoir by Mr. T. W. Edgeworth David and my 
 Colleague,t raised beaches occur in the delta of the Hunter River, New South Wales, 
 and reach to fifty feet above Ahe sea level. 
 
 I hold that a great submergence of the eastern coast (as exemplified by Sydney 
 Harbour and the Townsville Deep Drifts) was, at a comparatively recent date, succeeded 
 by a movement of elevation, which is still in progress. 
 
 No evidence of a Post-Tertiary Glacial Period has ever, so far as I am aware, been 
 met with in Queensland, unless the presence of temperate plants on some of our tropical 
 mountains be taken to afford the necessary proof. It is not improbable, however, that 
 evidence may yet be found in the southern ranges of the Colony of an approach to the 
 climatic conditions which prevailed in South Australia and perhaps in Victoria and the 
 southern parts of New South Wales (Mount Kosciusco). 
 
 Professor Ralph Tate, in a Paper read before the Australian Association for the 
 Advancement of Science at its meeting in Sydney in 1888,{ described certain glaciated 
 surfaces on the shores of Hallett’s Cove, in St. Vincent Gulf, a few miles from 
 Adelaide, in the following terms :— 
 
 “The glaciated surface, which I announced in 1877 as well developed ‘on the 
 coast cliffs at Hallett’s Cove, south of Holdfast Bay in St. Vincent Gulf, remains as 
 yet unique; but once it is accepted as of glacial origin, many other features obscure in 
 themselves acquire co-ordinate value in relation therewith. It is not my purpose to 
 describe the various signs which now can safely be attributed to glacial action, but 
 simply to bring to your notice tangible evidences of the glaciated condition of the rock 
 surface at Hallett’s Cove, and of its associated moraine débris. Actual inspection 
 would, I am sure, convince you. 
 
 
 
 * The north head of the mouth of Brisbane River. 
 + Rec. Geol. Survey of N. S. Wales, 1890, ii., 2. 
 * Proc. Austr, Assoc. Adv. Sci., 1890, i., p. 231 
 
 
 
619 
 
 “The path of the glacier is traceable for a distance of two miles along the top 
 of the scarped sea-cliffs at about forty feet above the sea-level; on the worth, it is cut 
 out from the cliff by encroachment of the sea; from this point ie glaciated surface is 
 continuous in a southerly direction for a Aine of one mile to Black Point, the 
 north headland of Hallett’s Cove. On the line of the glacier there now invervenes the 
 broad but shallow bay of Hallett’s Cove, but on the south headland the track is picked 
 up on about the same trend, though apparently at a little higher level—here again the 
 glacier path is soon cut out by removal of the cliff. 
 
 “On the north side of the Cove the glaciated surface is beautifully displayed, 
 the edges of nearly vertical strata are sheared off, and when of quartzite the surface 
 shows a high polish, and when of mudstones conspicuous grooves and strie. Some 
 moraine débris, including stones that have been beneath the glacier, occur here. On 
 the south side moraine matter is very abundant, and includes many boulders, some 
 occurring as blocs perchés. 
 
 “‘The common rocks of the morainic débris are granites, gneiss, hornblende- 
 schists, and others, which do not occur iz situ nearer than the gorge at Normanville, 
 about forty-six miles to the south. In all seventeen distinct varieties of rock, chiefly 
 metamorphic, and foreign to the immediate neighbourhood, have been collected along 
 the path of the glacier. 
 
 “The proximity of the Miocene escarpment suggests the possibility of the Pre- 
 Miocene age of the glacier. The Miocene fore ationt throughout its whole length on 
 this part of the coast has a conglomerate base consisting of well-rounded Sane of 
 limestone and quartzite and flat pebbles of slaty rock, but none other than local 
 material has been yet observed, though diligently searched for. It is highly probable 
 that the glacier cut its way through the incoherent Miocene formation, and that some 
 of the Miocene shingle furnished some portion of the moraine débris. 
 
 “Some measure of the antiquity of the glacier is further afforded by the amount 
 of marine erosion that has subsequently taken place. Assuming that the glacier was 
 in an alignment with the two headlands of Hallett’s Cove, then a length of three-fourths 
 of a mile by a breadth of one and a-half furlongs, and a thickness of forty feet, has 
 been removed since the glacier ceased to exist.’ 
 
 The correctness of Professor Tate’s observations has been called in question by 
 Mr. Gavin Scoullar,* Professor Hutton,t Dr. Lindenfeld,t and others, but the two 
 latter gentlemen, at least, have not seen the place. 
 
 An opportunity having occurred, I visited the locality, in company with Professor 
 Tate, in March, 1891. As it was my almost daily occupation for at least ten years, 
 when engaged on the Geological Survey of Scotland, to map the direction of glacial 
 striz, I may, without vanity, lay claim to some knowledge of the subject. I came to the 
 conclusion that Professor’s Tate’s observation was correct in every particular, and, in 
 addition, satisfied myself that the movement of the ice must have been from south to 
 north. There are certain little niceties of observation which enable one to judge of 
 the direction of the movement of an ice-sheet when producing polished surfaces and 
 striations. Thus, for instance, in passing over a slight fissure, the sharp edge of the 
 solid angle formed by the planes of the surface and of the side of the fissure will be 
 polished on the side furthest away from the motive force, while the edge on the other 
 side of the fissure will not be interfered with. Professor Tate has never committed 
 himself to an opinion on this point, although he expressed himself as satisfied with the 
 
 * Proc. Roy. Soc. South Australia, 1884-5, p. 46. 
 + Quart. Journ. Geol. Soc., xli., p. 218. 
 t Proc. Linn. Soc. N. S. Wales, x., p. 2. 
 
620 
 
 evidence which I pointed out when on the spot. A movement from south to north 
 accords very well with Professor Tate’s own observation that “the common rocks 
 of the morainic débris are granites, gneiss, hornblende-schists, and others, which do 
 not occur in situ nearer than the gorge at Normanvyille, about forty-six miles to the 
 south.” 
 
 Naturally, it seemed reasonable to suppose that a local glacier must have 
 produced the roches moutonnées and striz, but, on the other hand, there are no mountains 
 in the neighbourhood of sufficient altitude to give rise to a glacier of such importance as 
 to fill the whole broad valley occupied by St. Vincent Gulf. It is equally true that 
 there is no sufficiently high land to the south. It is possible, but not probable, that 
 such high land may have formerly existed either to the north or south, and have 
 subsequently been depressed. Violent as the supposition may be, it is more likely that 
 an Antartic ice-cap extended as far as the southern coast of Australia. South of 
 St. Vincent Gulf, and west of Tasmania, an oceanic depth of over twelve thousand feet 
 is speedily reached, and in sea-water of this depth ice of nearly seventeen thousand 
 feet in thickness would float without grounding. These figures may be supposed to 
 reduce the argument in favour of an Antartie ice-cap ad absurdum. Be this as it may, I 
 regard it as an ascertained fact that a sheet of ice moved from south to north up 
 St. Vincent Gulf. 
 
 As bearing on the question of the possible extension of an Antartie polar ice-cap, 
 some pregnant observations were made during the Scientific Voyage of the “ Challenger.”’ 
 Not having it in my power to refer, as I write, to the “Challenger” reports, I am compelled 
 to quote, at second-hand, from some comments thereon by Mr. G. S. Griffiths, F.G.S.,* 
 relating to evidences of a Glacial Period from Kerguelen Land. 
 
 Kerguelen Land is situated in the Indian Ocean, approximately in Long. 70° 
 E., and Lat. 50° S.—i.e., about 15° south of the latitude of Adelaide. It may 
 be remarked, further, that it is just south of Kerguelen Land that the curve 
 denoting the northern limit of (Antartic) drift ice recedes nearer the pole than in 
 any other portion of the Southern Hemisphere. The curve is denoted on physical 
 maps as keeping about 10° or 12° south of the Australian Continent, and about the 
 same distance south of Kerguelen Land, although the latter is quite 15° further south 
 than the former. For a continental ice-cap to reach Australia from the southern polar 
 regions would be no more remarkable, therefore, than for one to reach Kerguelen 
 Land. In other words, the change of temperature required to bring about the 
 one would suffice to bring about the other. That the evidence of a Glacial Epoch 
 in both places is much of the same character will be evident from the following 
 extract :— ; 
 
 “ The interesting feature in relation to these glaciers is that, whereas they are 
 to-day confined to the higher valleys of the higher ranges, there are abundant and 
 indisputable evidences that the whole island down to and even below the sea-level was 
 buried under ice at a comparatively recent period. The furrows of glaciers are seen 
 wherever the island has been explored. The lower hill-tops, still bare and barren, have 
 been cut down by travelling ice, which has planed them smooth, exposing clean-cut 
 horizontal sections of the geodes of the amygdaloidal rocks. Each shelf of the basalt 
 stairs has its strie, and the lower valleys are scratched and scraped and smoothed by 
 glaciers which have since disappeared. Every harbour is an ice-cut fiord.t” It may be 
 remarked that the whole island being buried under ice is apparently inconsistent with 
 the idea of local glaciers. 
 
 
 
 
 
 * Trans. R. Soc. Victoria, xxiii. 
 + ‘* Challenger ” Reports, p. 356, 
 
 
 
 
 
 
 
621 
 
 If an Antarctic ice-sheet actually impinged upon the shores of the Great 
 Australian Bight, we may expect to hear of the discovery in Victoria of glaciated 
 surfaces similar to those of St. Vincent Gulf, although, perhaps, the soft and incoherent 
 Tertiary rocks of which a great part of the southern coast-line is composed may be 
 unfavourable material for the retention of markings. 
 
 The evidences of former glacial action are thus succinetly summed up by Mr. 
 James Stirling, F.G.S., F.L.8.* :— 
 
 “ Erraties in the Mitta Mitta and the Kiewe Valleys, huge blocks weighing many 
 tons ; smoothed surfaces on the Cobberas Mountains and Mount Bogong; morainics at 
 the base of the latter on the Mountain Creek Valley; eroded lake basins, Dry Hill, 
 Hermomugee Swamp ; Omeo lake basin; morainie lake, Mount Wellington; smoothed 
 and scratched surfaces on Mount Kosciusko. The interest appertaining to this question 
 is no doubt great, and although the fact of glacier action can, I think, be satisfactorily 
 established in the Australian Alps, yet further evidence is desirable as to the synchronism 
 of the glacier period in Australia with that of the glacial epoch in the Northern 
 Hemisphere. That the glacier action was widespread over South-east Australia, I have 
 no doubt, and without entering into a discussion as to the causes of such glacier action, 
 it seems to me difficult to resist the conviction that, considering the uniformity of 
 natural operations all over the globe during past time, Australia was not exempt from the 
 refrigeration which in the Northern Hemisphere culminated in a glacial epoch. The 
 geological evidences are, I think, accumulating in favour of the view that glacier action 
 has played a very important part during Mesozoic and Paleozoic time in the distribution 
 of boulder deposits and the abrasion of rock surfaces. Mr. Dunn, F.G.S., has recently 
 found some well-marked striated boulders in the Older Tertiary conglomerates in the 
 Beechworth district, which may be seen at the Melbourne Centennial Exhibition, while 
 the author has found similarly striated boulders in the Upper Silurian conglomerates 
 of the Gibbo River.” 
 
 To the most recent phase of the Post-Tertiary, and extending to the present day, 
 belong the accumulations of Blown Sand, or Dunes, which fringe the coast at intervals 
 from Cape Moreton to Cape York. In some cases the Blown Sand attains a considerable 
 elevation, but this circumstance must be attributed to such conditions as force and 
 direction of the wind, slope of the land, &c., and not to upheaval. 
 
 Blown Sand occurs at the north end of Moreton Heads, and all along the western 
 or sheltered side of Moreton Island, at a height of about 150 feet above the sea. 
 
 At Double Isiand Point, near the south end of Fraser Island, the late Rev. J. E. 
 Tenison Woods referred} to ‘‘a formation of sand which forms cliffs for some three or 
 four miles,’ and adds that the sand cliffs “‘are densely covered with a light brush 
 (Melaleuca genistifolia?). The cliffs of sand are quite precipitous on the seaward side, 
 and are from 100 to 200 feet high. On a close examination, the cliffs present exactly 
 the appearance of the Hawkesbury Sandstone, except in colour, and they are not 
 consolidated.t{ There are the same undulating ‘layers,’ of varying thickness, forming 
 thick sinuous marks upon the cliffs, which can be seen at a great distance. The layers 
 are entirely constructed of lamine of sand, with false bedding, which dips at every angle 
 not outside 30°. The layers are of different colour, and they seem to preserve 
 this colour throughout, giving the cliffs a curious ribbon-like structure. Some are white, 
 
 * The Physiography of the Australian Alps. Proc. Austr. Assoc. Adv. Sci., i., 1889, p. 359. 
 
 + The Hawkesbury Sandstone. Journ. Roy. Soc. N. S. Wales for 1882 (1883), xvi., p. 53. 
 
 +The Author argued that the Hawkesbury Sandstone is of zolian origin, and mentioned the sand- 
 dunes of Double Island Point in illustration of the theory, which is inconsistent with the fact of the 
 discovery of fish-remains in the Hawkesbury Sandstone, and with many other observed facts, 
 
622 
 
 others yellow, and some ochreous red. The formation is entirely one of blown sand. 
 On the surface, where ti-tree brush does not grow, the sand forms the usual shifting 
 dunes of rounded outline and great height. In places there are sand-slips on some of 
 the dunes, where the false bedding becomes revealed. The undulating lines which 
 separate the various layers are found to consist of decaying vegetable matter, or rich 
 loamy earth with roots, leaves, and land shells intermingled. They represent the former 
 surface of the drifting sand, where its shifting has been stayed by the growth of a dense 
 brush. Thus it has remained stationary for years, until a change of wind, or, perhaps, 
 a bush fire, has brought the sand on to the surface again and overwhelmedit. In part of 
 the brush there are swamps of water; at least, so I was informed. a 
 
 Sand-dunes occur near Mackay, between East Point and Armhurst, “ forming 
 hillocks of no very great height and of which the landward slope is much steeper than 
 that facing the sea.’’* 
 
 North of Townsville, in the Town Common, and south of Townsville, between the 
 mouths of the Ross River and Alligator Creek, the Raised Beach is covered in places by 
 three or four parallel ridges of blown sand which sometimes attain a height of thirty feet. 
 
 In Shelburne Bay, Cape York Peninsula, sandhills occur at a considerable 
 elevation, and enclose a circular lagoon of fresh water about a quarter of a mile in 
 diameter.t ‘ 
 
 In Temple Bay, the Raised Beach already referred to as occurring north of 
 Camisade Creek is partly covered by blown sand, which extends for a considerable 
 distance inland and attains an elevation of nearly four hundred feet. 
 
 Sandhills stretch inland for a considerable distance from Orford Bay, attaining 
 a height of three hundred feet in places.t 
 
 HAS MAN A GEOLOGICAL HISTORY IN QUEENSLAND? 
 
 The answer to this question may be given in one word—No. That is to say, 
 so far as I am aware, no evidence of the presence of Man, or of his works, has yet been 
 discovered in any raised beach, cave, or stratified deposit associated with the remains of 
 extinct animals. 
 
 The question “ Has Man a Geological History in Australia?’’ has been discussed 
 at length by my Colleague in the Proceedings of the Linnean Society of New South 
 Wales.§ His conclusion is as follows :— 
 
 ““(1) Up to the present, as at the time Mr. R. B. Smyth wrote, the existence of 
 Man’s works in any geological deposit, above question, has not been shown to exist. 
 (2) The molar crown found in the Wellington Breccia Cave appears to be that of a 
 human being, and is to all intents and purposes a fossil. (3) Its position in the cave 
 and association with the other organic remains there entombed is open to doubt. 
 (4) No other human remains have been found at Wellington under similar conditions. 
 
 “The mineralized condition of the tooth is, of course, its strongest recom- 
 mendation ; but I do not think that, in a momentous question of this kind, and one on 
 which so much theory can be built up, this should be allowed to outweigh other 
 evidence pointing in a different direction. 
 
 “The matter can hardly be summed up better than by the very reasonable and 
 often correctly applied Scotch verdict of ‘ Not proven.’ 
 
 
 
 * Report on the Geological Features and Mineral Resources of the Mackay District, by A. Gibb 
 Maitland. Brisbane : by Authority : 1889. 
 ; + Report by R.L.J. on Explorations in the Cape York Peninsula, 1879-80. Brisbane: by Authority : 
 1881. 
 
 eae hivehs post 
 
 § 1890, v., (2), p. 259. 
 
 
 
623 
 
 “Tn conclusion, I woud distinctly wish it to be understood that I have not lost 
 sight of the bearing the relative antiquity of the Tasmanian Aborigines has on this 
 subject. The former geological connection of Australia and Tasmania now appears 
 to be a generally accepted fact. The late Mr. James Bonwick regarded* the Tasmanians 
 as an older race than the Australians, although emanating from a common centre, and 
 dispersed over a then existing continent of which our present Australia and Tasmania 
 formed portions. If such be the case, how vast a period of time must have elapsed 
 since then, allowing for the formation of the channel we now know as Bass Straits ; 
 and herein lies one of the strongest proofs of Man’s early existence on the Island 
 Continent of Australia. Notwithstanding this, however, there remains the undoubted 
 fact that we still lack trustworthy geological information of the approximate date of 
 his first advent in Australia.” 
 
 Professor Ralph Tate, on the other hand, would assign to Man in Australia 
 an age as far back as Pliocene. Speaking of the volcanic district of the south-eastern. 
 portion of South Australia (Mount Gambier, &.), he says +:— 
 
 “The Pliocene sands and loess of this place are of terrestrial origin; they contain 
 remains of Diprotodon, Phascolomys pliocenus, McCoy; and leaves of Casuarina and 
 Banksia are imprinted on the under surfaces of the superimposed ash layer. 
 
 “ Did Man witness the showers of ashes and the glow of the internal fires of these 
 cones reflected from the clouds? Probably, Yes! . . . The dingo (Canis dingo) was 
 the contemporary of the Diprotodon, whose remains are buried beneath the ashes of the 
 Mount Gambier volcano, as proved by their remains occurring together in the Gisborne 
 and Wellington Caves. 
 
 ‘“‘ Now, the dingo is an alien; he forms no part of the Australian fauna; and his 
 introduction by Man, as a companion and assistant in the chase, can only satisfactorily 
 explain his presence in this continent. Man and dog may have pursued together the 
 Diprotodon, and in later times have been awed by the volcanic outbursts. Indeed, no 
 other cause of extirpation of the huge mammals has suggested itself.to the mind of 
 ‘Professor Owen, save that of human agency. He says, ‘To a race of men, depending, 
 like the blackfellows, for subsistence on the chase, the largest and most conspicuous 
 kinds of wild beasts first fall a prey.’ ” 
 
 I am quite willing to admit that the Dingo is an “alien”; but it is open to 
 question whether the agency of Man was the only possible means of effecting his 
 introduction into this island. The Dingo is a wily animal, full of resource and self- 
 reliance, and very different in this respect from the domesticated dog, which appears to 
 have to some extent lost the habit of independent action, as it is well known that many 
 dogs will suffer agonies of thirst rather than go to the nearest water, unless their 
 masters take them out “ for a walk.” The Dingo, as we know him to-day, is capable of 
 taking care of himself, and he or his ancestors may have arrived in Australia by some 
 chance means of conveyance without assistance, or may have simply walked overland. 
 It is quite possible, therefore, that he may have been contemporary with the Diprotodon, 
 and have witnessed the ash showers of Mount Gambier without having had his emotions 
 shared by a human companion. f 
 
 
 
 * J. Bonwick. Daily Life and Origin of the Tasmanians, 1870, p. 259. 
 
 + Anniversary Address to the Royal Society of South Australia, for 1878-9. 
 
 + There is not a fragment of evidence to show that the arrival of Man was‘coeval with that of the Dingo, 
 On the contrary, the absence of authenticated remains of the former with those of either the Diprotodon or 
 Dingo points rather the other way. It is not even certain that the bones of the Dingo have been found in 
 the Wellington Caves. On the other hand, the late R. Brough Smyth states that the remains of the Dingo 
 have been found under “ volcanic ash some thirty or forty feet in thickness.” If my memory does not 
 deceive me this was at Towerhill, Warrnambool. (RZ. Junr.) 
 
624 
 THERMAL AND OTHER SPRINGS. 
 
 It is desirable to record in this place such information as we have on the subject 
 of the Thermal and other Springs which break out, chiefly, in the Western Interior. 
 The subject is closely connected with Artesian Wells, as has been remarked in a previous 
 chapter. 
 
 Further notes on the springs which break out at the base of the Desert 
 Sandstone will be found in Chapter xxxiii. (p. 518). 
 
 Mud Springs, Hamilton River.—Mud springs break out in many places between 
 the channels of the Hamilton River (Lat. 23° 20’ S., Long. 140° E.). These are 
 described by a writer in the Townsville Bulletin® as “miniature volcanoes casting out 
 liquid mud instead of lava.’ In several bores in this neighbourhood Artesian Water 
 has been met with at shallow depths. 
 
 Hot Mud Springs, Flinders River—Daintree, in his “ Notes on the Geology of 
 Queensland,” + described as follows the hot spring on the Saxby River :— j 
 
 ‘“‘ At Gibson’s Cattle station, on the Saxby River, a tributary of the Flinders, a 
 spring of hot water rises above the surface of the plain; and its overflow deposits a 
 white incrustation, which, on analysis by Dr. Flight, under the direction of Professor 
 Maskleyne, afforded :— 
 
 Water... ine i ca BS ae ae #5 sn CV PEEE 
 Silica Ase ai see Set see ae ME ais ...  0°600 
 Chlorine ... aa Ae wae aes ips mie ose Ap eset, 
 Sodium ... fae ven aad ha a vas sat Rom | rapists: 
 Carbonic acid Ake ae ace ae vee — oe se OO 78D 
 Soda sg cae ae sae ies re ome a soo, ont] 8) 
 
 99°370 
 
 “The sulphuric acid, of which there was a small portion, was undetermined. 
 
 “ Apart, therefore, from the 5552 per cent. of chloride of sodium, the deposit 
 consists of sesquicarbonate of soda, or native Trona, and as such it is used by the 
 settlers for culinary purposes, &c.”’ 
 
 I do not gather from Daintree’s Paper that he had seen the hot spring referred 
 to; at least he gives no description. This is supplied by Mr. E. Palmer, M.L.A., in a 
 Paper on “ Hot Springs and Mud Eruptions on the Lower Flingers River.” t 
 
 Mr. Palmer remarks that the Springs “on the Lower Flinders occur in separate 
 clusters, each consisting of innumerable small eruptions, surrounding one or two large 
 central or main springs, within a radius of a mile or so, and all more or less in a state 
 of activity—that is, they emit streams of thin mud or water intermittently. They are 
 found on either side of the river, and seem to have no connection with, or influence on 
 the water in the river, which may be said to be only a surface water. Although 
 possessing a striking similarity to each other, still any connection between them must 
 exist beneath the present course of the Flinders, which is cut out of the level plains 
 by the annual tropical rains, and is a river of Recent times; no hollow or valley exists 
 where the course of the river runs; the banks are nearly perpendicular, but not 
 very deep, while the level plains extend right up to the bank of the river. The springs 
 belong to an older formation than present river system, and must derive their force 
 from some very distant inland mountainous country.” 
 
 
 
 * 23rd July, 1891. 
 + Quart. Journ. Geol. Soc., xxviii. (1872), p. 28 . 
 + Proc. Roy. Soc. Queensland, i., 1884 [1885], p. 19. 
 
 
 
625 
 
 After describing the course of the Flinders, Mr. Palmer continues :— 
 
 “The only elevations are Mount Browne, in about 20° south latitude, a low 
 stony rise of ironstone and granite, rising from the plain, and about a mile from the 
 river on the right side, and Fort Bowen, twenty miles west, similarly situated with 
 regard to the river, and rising also abruptly from the open plains. These are the 
 only rises of any consequence near the river, and at both of these small mountains 
 numbers of springs and mounds of erupted mud, coated with a whitish crust of soda, 
 lie scattered about, with stumps of large tea-tree and reeds, and pools of discoloured 
 water throughout; while at Mount Browne occur two hot springs on the south side 
 with a temperature of 120° Fahrenheit at the surface. The water stands in a large 
 basin on a mound raised many feet above the level of the plain, and covered with 
 gigantic tea-trees (Melaleuca leucadendron), amongst the matted roots of which the 
 hot water streams in clear, shining, crystal pools. The basin, or cavity, is fathomless, 
 while the roots and branches lying in it are coated with a soft, green vegetable 
 matter with air-bubbles attached, small bubbles of carbonic acid innumerable, which 
 are continually rising to the surface. The water is too hot to bear the hand in for 
 any length of time; but when cooled is good for use, and always bright and clear 
 and free from any taste, while*that in the adjoining cold springs is extremely dis- 
 agreeable. No change has been observed in the hot springs in level or temperature 
 since 1865, when a cattle station was settled there by Mr. James Gibson.* The ground 
 round all these springs is treacherous, is hollow, shakes to the tread, and feels like a 
 huge blister, merely covered with a skin of soil, held together by roots and rushes, over 
 which one can walk. At times the pressure from below forces the thin crust upwards, 
 and a flow of this brown liquid mud spreads about, sometimes in great quantities. In 
 one of the springs at Mount Browne, flakes of granite are forced up and lie on the 
 surface. It seems as if a connection existed down by the side of the mountain to subter- 
 ranean regions, whence the hot water flows, and is kept at one constant level and 
 temperature. Most of the mud springs have formed large mounds, or cones, by constant 
 overflow, and the water now stands at the top, while the surrounding parts are spongy, 
 and liable to break through when stock comes near them; at others lagoons are formed, 
 and kept at a uniform level by the flow of water. The occurrence of these hot and cold 
 mineral springs suggests the possibility of obtaining supplies of water on the artesian 
 principle over some portion at least of these extensive plains. Some mud springs, as 
 they are called, opened at Manfred by a small shaft at ae side, produced a permanent 
 flow of good water. 
 
 “Fresh ground keeps continually breaking up, or is forced up, while old cones 
 are sometimes falling in, forming holiows half- full of reddish water, strong as lye, and 
 quite undrinkable. None of the springs are isolated, but confined to the vicinity of 
 one or other of the half-dozen groups which compose the collection on the Lower 
 Flinders. The direction of these groups is in a north and south course from each 
 other, with the Flinders River dividing them, and they are comprised within a line or 
 distance of eighty miles. Above Dalgonally Station, on Julia Creek, some very extensive 
 mounds are an indication of the force of the pressure from below, while an open 
 spring between it and the Flinders has numerous small fishin it. A thoroughly scientific 
 description of these numerous and wonderful displays of natural forces would prove 
 very interesting and instructive. The vegetation surrounding them is peculiar, and 
 somewhat distinct from that of the plains. The locality of any of the groups of mineral 
 springs is indicated by the presence of gigantic ti-trees surrounding them, and many 
 
 *I think there can be no doubt that this refers to the same Spring as that referred to by Mr, 
 Daintree. (2.L.J.) : 
 2Q 
 
626 
 
 of the mounds present a pleasing green appearance, from being covered with a sward 
 of Fimbristylis, in such masses, fallen or recumbent, as to form a safe carpet, yielding 
 and soft, but dense enough to support cattle going in to feed on the various grasses 
 found there. 
 
 “In ancient days the same springs have proved a trap for too-confiding animals, 
 as is proved by the fact of some bones having been ejected in the mud from one of 
 them; the bones are coloured, but in a good state of preservation.” 
 
 On the Gilliat River, a tributary of the Cloncurry, below the junction of Eastern 
 Creek, some mud springs are marked on the ‘“‘Sixteen-mile Colony Map,” but I have 
 neither seen nor been able to obtain any description of them. 
 
 Einasleigh Hot Springs.—I visited these Springs in November, 1889, in company 
 with Mr. A. Gibb Maitland. 
 
 The Springs have been known for about eighteen years, but the knowledge was 
 for a long time confined to the station hands. Of late years, however, a few pleasure 
 parties have gone out to visit them from Georgetown, the centre of the Etheridge Gold 
 Field, from which they are distant about forty-five miles, and, since the opening of 
 Croydon Gold Field, in 1886, a few rheumatic and other invalids have camped on the 
 Einasleigh and bathed in the hot water. Mr. C. A. Vogan read a Paper on the Springs 
 in September, 1888, before the Geographical Society in Sydney. 
 
 The Springs are best reached by following the river down from Cobb and Co.’s 
 Stage on the coach road at the crossing of the Hinasleigh. As the left bank of the 
 river is flanked by rough broken country for some distance, it is best to keep the right 
 bank for three miles and then cross to the left bank. The crossing presents no difficulty, 
 as although the river is here nearly a hundred miles from its source and almost half-a-mile 
 wide, its bed is, in ordinary seasons, a sandy waste, only relieved by occasional 
 waterholes. 3 
 
 About six miles below the road the traveller is guided to the Springs by a small 
 cloud of vapour rising from a mound partly concealed by trees in the middle of an 
 alluvial flat, and distant about a quarter of a mile from the left bank of the river. 
 
 On closer inspection the mound proves to be a dome-shaped mass fifteen feet in 
 height and two hundred yards in circumference, rising out of a plain of recent alluvial 
 deposits. That the latter are of no great thickness is shown by sections on the river 
 banks and in gullies, which expose gneiss, granite, and schists very near the surface of 
 the plains. 
 
 Scattered over the dome are five distinct springs of clear, blue water, all of 
 which, with one exception, leak quietly over their: rims without ebullition or geyser 
 action. 
 
 The story runs that about nineteen years ago the Georgetown Mailman heard, 
 from a distance of two or three miles from the Springs, an explosion and a hissing noise 
 like that of escaping steam. Little notice was taken of this report at the time, buta year 
 later the Springs were found in the locality indicated by the mailman. If the story is 
 true, it would appear that the Springs really do burst into geyser activity at rare intervals. 
 
 The apex of the mound is occupied by a sheet of water which measures roughly five 
 by three feet across the mouth of a well which has a depth of six feet (Spring a). This 
 Spring discharges by one principal and two minor breaks in the lip of the cup, streams 
 having an estimated total section of nine square inches. Bubbles of gas continually rise 
 to the surface, but at intervals of two and a-half minutes there is a rush of bubbles. 
 
 Eighteen feet north of (a), a pipe (2) of one foot in diameter is filled with seven 
 feet of water, which does not rise to the surface of the mound nor discharge by any 
 visible orifice. From the surface of the mound to the surface of the water is two feet, 
 
627 
 
 and the cup is continued from the water-level upward, in funnel shape, the funnel 
 measuring about three feet across the top. The surface is about five feet below the 
 tevel of the apex of the mound. Gas-bubbles rise slowly through the water. 
 
 Fifteen feet north of (4) is a third well (Spring c), measuring six by four feet 
 across the top, which is about the same level as that of Well (J). The water is three and 
 a-half feet deep, and stands about six inches below the lip, but discharges to the north a 
 stream, estimated at thirty-six square inches, two feet below the level of the lip. Gas- 
 bubbles rise slowly through the water. 
 
 Twenty feet east of (a), a fourth well (Spring d@) is three feet in diameter at the 
 surface, which is on the same levelas (4) and (c). The water, which is seven feet deep, 
 escapes at the surface in a stream estimated at nine square inches, and at the base of the 
 mound—.e., ten feet below the surface level of the water—in a stream estimated at a 
 hundred and forty-four square inches. Gas-bubbles rise slowly through the water. 
 
 The lowest well (Spring e) is full to the lip, which is about seven feet below the 
 apex of the mound. Bubbles of gas rise constantly, but irregularly. The cup is very 
 irregular in shape, but is, roughly speaking, about twenty-five by fifteen feet across. The 
 depth of water over the greater part is only three feet, but one portion, about five feet in 
 diameter, is of greater depth—probably six or seven feet. The water leaks out over the 
 rim in every direction, but chiefly towards the west, in streams with an estimated total 
 sectional area of four hundred square inches. 
 
 The water in all the wells was too hot to touch, evidently not far from the 
 boiling point; but, as I had no thermometer, I was unable to ascertain its exac 
 temperature, Its taste, when cooled, was indescribably nasty, resembling what one 
 could imagine to be that of water in which very much decayed fish had been boiled. 
 The gaseous emanations from the largest well smelt distinctly of sulphuretted hydrogen, 
 and twice only [ got a whiff as of sulphur. A quantity of the water from Spring (d) 
 was bottled and sent to the Government Analyst, whose report is as follows :— 
 
 * Carbonates of calcium and magnesium .., vee sr aE ... 6°25 grains per gal. 
 Carbonates of sodium and potassium ... sas op ae eee Lo; 04 wee. 
 Chloride of sodium and potassium Ay vei ae Ae wos 6b 75 is 
 
 Total fixed salts .., Pn ais Ase Pe nee 500 ERS) ap a 
 Volatile matter ... tee “fr oa i 5 waa o0 ” 
 Total solids... oe pte va ‘ee = ... 57°60 
 
 Sulphuric acid, trace. 
 Sulphuretted hydrogen, 2°19 grains per gallon. 
 
 “ The same is a chlorinated sulphuretted water, and possesses similar medicinal properties to that 
 of Harrowgate (England), but in a lesser degree—to the extent of about one-seventh of the Harrowgate 
 Le “Roper Mar, F.O.8., Govt. Analyst.” 
 
 Little less than the want of a thermometer did I regret the want of a bar of 
 soap, with which I could have tried the experiment which has been successfully 
 carried out in the Yellowstone Park (to such an extent, indeed, that it has become a 
 public nuisance). Perhaps the next visitor may go better provided, and succeed in 
 temporarily exciting the quiet springs into active geysers. Mr. Arnold Hague, of the 
 United States Geological Survey, in an article on “ Soaping Geysers,” read in February, 
 1889, before the American Institute of Mining Engineers, after detailing his experi- 
 ments on the ‘“ Chinaman,’”’ “Old Faithful,” ‘ Beehive,’ ‘‘ Giantess,” and other 
 geysers, accounts for the artificial ebullition as follows:—“ If soap or lie is thrown into 
 most of the small pools, a viscous fluid is formed ; and viscosity is, I think, the principal 
 cause in hastening geyser action. Viscosity must tend to the retention of steam within 
 
628 
 
 the basin, and, as in the case of the superheated waters, where the temperature stands 
 at or above the boiling point, explosive liberation must follow. All alkaline solutions, 
 whether in the laboratory or in Nature, exhibit, by reason of this viscosity, a tendency 
 to bump and boil irregularly.” It may be mentioned that the “ Chinaman,” like the 
 Hinasleigh Springs, is a mere hot spring, never seen in geyser action, except when 
 excited by soap. 
 
 Round the margins of all the basins we found a little rim of remains of dragon- 
 flies, beetles, Savers frogs, &e. These had the appearance of having been boiled, 
 and a slight deposition of carbonate of lime had, in some cases, taken place on their 
 harder parts. The deposition is evidently a slow proesss, some twigs, which had certainly 
 been a long time in the water, being “petrified” only in a trifling degree. It would be 
 interesting for a naturalist to ascertain how these animals met their deaths, but our time 
 did not permit of such an investigation. Did the dragon-flies hover over the surface of 
 the water, as is their custom, till they were overpowered by the gaseous emanations? 
 Did the frogs leap into the inviting blue water in ignorance of its deadly temperature ? 
 I may mention that I have seen frogs sporting in the warm water issuing from some of 
 the New Zealand hot springs. 
 
 The mound is composed of carbonate of lime, and is covered by semi-circular or 
 oval basins forming a series of steps from the summit to the edge of the dome. The 
 water overflowing from the wells pours into these cups one after another, and, 
 decreasing in temperature as it recedes from its source, the cups afford natural baths 
 in which an invalid may be immersed in water of any temperature he may fancy. 
 
 It is easy to see the cause of the formation of the cups in the comparative rapidity 
 with which the calcareous sinter would form round the edges of any accidental hollow in 
 which the water might lodge. The heightening and extension of the rim would gradually 
 enlarge the cup till it contained so much water that the tendency of the overflow 
 would be to wear one channel deep enough at last to drain the cup. 
 
 The calcareous sinter is light and spongy on the surface, but is tolerably compact 
 in the interior. Loose in the bottom of the dry cups are shovelfuls of needles and 
 spikes of calcite, each an ag gregation of rhombohedral crystals. It may be remarked 
 that the deposits of hot springs in other parts of the world are much more commonly 
 siliceous than calcareous. 
 
 It must be confessed that there is little of the picturesque in the general 
 appearance of the mound, which is not striking for its size, and is of a dirty white or 
 drab colour ; but, to the eye capable of dissociating colour from form, some of the cups 
 are exquisitely beautiful in the freedom and originality of their curves. In this 
 respect, at least, the Einasleigh mound and terraces will compare favourably with 
 anything of the kind remaining in New Zealand since the destruction of the Rotomahana 
 Terraces by the eruption of Tarawera. 
 
 Not the least singular thing about the Springs is the stream formed by their 
 overflow. It gives rise to a narrow swamp on the surface of the alluvial flat, and runs 
 parallel with the bank of the river for about half-a-mile. The bulk of the water 
 empties into the river at the far end of the swamp, but portions of it form two distinct 
 gullies discharging into the river nearest the Springs, and two still higher outlets, though 
 now dry, evidently at times convey part of the stream. Whether this points to an 
 increased flow from the Springs at times, or whether the volume of water in the swamp 
 is simply increased during wet seasons, I cannot say. 
 
 It is in the highest degree unlikely that five distinct hot springs should rise from 
 unknown depths to escape within an area which can be compassed by two hundred and 
 sixty paces. It is much more probable that there was originally a single orifice, which 
 
629 
 
 was gradually choked up by the deposition of sinter till it became insufficient for the 
 passage of the water. The water would then have to find other outlets; though it is 
 quite possible that a much greater volume of water would overflow if the deposit of 
 sinter were removed eitber violently by a “ convulsion” or by artificial means. 
 
 Assuming (as we may with safefy) that the “bed-rock” on which the sinter 
 mound is built up is not ten feet beneath the surface of the surrounding alluvium, we 
 have a cone of known dimensions, and could roughly estimate the time required for the 
 formation of the cone, knowing as we now do, from Mr. Mar’s Analysis, the amount of 
 lime and other salts held in solution by the water, and the amount of water discharged by 
 the wells, if observations were carefully made to show the amount of solid matter held 
 in solution by the water escaping beyond the limits of the mound. Here again, 
 however, we should have to assume that the discharge of water was always the same 
 as now, whereas it is probably diminishing, so that we should get as a result only a 
 minimum time. 
 
 It now remains to consider the evidence bearing on the geological age of the 
 Springs. | , 
 
 In a section from the Etheridge to the Hinasleigh, taken on the level of the two 
 rivers (both about 1,200 feet above the sea), mica-schists, gneisses, and granites alone 
 would be met with. The mica-schists probably represent sedimentary rocks of 
 pre-Devonian age, although Iam not aware of any direct evidence to that effect; and 
 the gneisses and granites, metamorphosed rocks of like origin and age. ‘The granite 
 largely predominates along the supposed line of section. But above the level of the 
 two rivers, the Newcastle Range has been built up, from an elevation of 1,920 feet at 
 its base to 2,240 feet near its summit, of a coarse angular volcanic agglomerate. On 
 this rests a cake of Desert Sandstone (Upper Cretaceous), perhaps a hundred feet in 
 thickness. A strictly parallel section is seen on crossing the Newcastle Range by the 
 Townsville and Georgetown Road twenty-five miles to the south. 
 
 Large sheets of basalt occupy the bed of the Einasleigh and surrounding 
 country where the river is crossed by the Townsville and Georgetown Road, and, lower 
 down the valley, basaltic cowlées are found overlying the older alluvial deposits, having 
 been poured down the valley over the bed of the river, which at length cut through or 
 found its way past the edge of the basalt. Similar fragments of basaltic coulées, it may 
 be mentioned, occupy portions of the valleys of Surprise Creek and the Lynd River, on 
 the road from Georgetown to Herberton. 
 
 It was after the denudation of the Desert Sandstone (Upper Cretaceous) and sub- 
 jacent rocks had been carried on by the Hinasleigh to the depth of a thousand feet that 
 the lava-form basalts burst out and flowed down the valley. Probably no inconsiderable 
 portion of Tertiary time was occupied by this stupendous amount of denudation; and 
 it is more than probable that the volcanic forces which produced the outbursts of 
 basalt may still, though diminishing, possess sufficient vitality to give rise to thermal 
 springs. 
 
 Jn all likelihood, the EHinasleigh Springs broke out in the bed of the river 
 immediately after the denudation of the basalt—in the bed of the river by preference, 
 because there the pressure of superincumbent rock offered the least resistance. The 
 building of the sinter-mound would keep pace with the formation of the alluvial terrace 
 when the river subsequently altered its course. In modern times the sinter is probably 
 overlapping the alluvium. 
 
 Innot Creek Hot Springs.--These Springs are about twenty-eight miles from 
 Herberton, a coach running once a week. A hotel has been built for the accommodation 
 of visitors, 
 
630 
 
 Mr. Ludgwig Bruck, in an Article on “The Mineral Springs of Australia,”* 
 gives the temperature of these Springs as 189° F., and says:—“The waters taken 
 internally have an aperient action ; but patients undergoing treatment combine bathing 
 with the drinking of the waters, two or three baths of a duration of twenty to thirty 
 minutes being taken daily. These Spring’ have already gained a considerable 
 reputation for their curative virtues in chronic rheumatism, gout, liver, and kidney 
 diseases; but like Karlsbad,in Bohemia, the most celebrated Thermal Spa in Europe, 
 the Innot Hot Springs should also be invaluable in catarrh of the stomach and intestines, 
 dyspepsia, constipation, dysentery, diseases of the genito-urinary organs, hemorrhoids, 
 sterility, &. The principal spring in Karlsbad is the ‘ Sprudel,’ with a temperature 
 of 170°, or 19° lower than the Innot Springs, while in mineral salts the Karlsbad Springs 
 are considerably richer.” 
 
 Mr. A. Gibb Maitland, in a report on “ The Coolgarra Tin Mines and Surrounding 
 District,” + says :—“ Between Gunnawarra Station and the Hot Springs, near Woodleigh, 
 the road passes over rather flat sandy country, with scarcely a section visible. Probably 
 the underlying country is granite. Within four miles of the Hot Springs, portions of the 
 country are occupied by basalt. In the vicinity of the Hot Springs, the prevailing 
 country rock is a granite of variable composition and texture, intersected by dykes of 
 felsite and a rock not unlike a quartzite in appearance. 
 
 “The Springs are situated in the bed of Innot’s or Nettle’s Creek, a tributary 
 of the Herbert River, and about two and three-quarter miles north-west of Woodleigh 
 Station, at an altitude, by Aneriod, of 120 feet above Gunnawarra, or about 1,900 feet 
 above sea-level. 
 
 ‘Tradition has it that some years ago the present site of the Springs was occupied 
 by a large waterhole full of and overflowing with hot water. 
 
 “ The only analysis of the water which is believed to have been made is that by 
 the late Mr. Karl Staiger, sofmetime Government Analyst, who reported that the sample 
 analysed by him contained 61°126 grains of solid matter in one gallon, viz. :— 
 
 Chloride of sodium BY: a sks A nee ae «625245 
 Alumina and iron ae Sa ary, ane wee ae .. 2°057 
 Carbonate of lime ane a a ce she see vee «= 2304 
 Sulphate of lime,,, Th ee 38 ne re mea ... 6230 
 Silica awe Att ah ae ai ane aes vee OL 
 Insoluble solids ... fae ine ae fr aa nee ... 16040 
 Organic matter ... re oa mod aa “ne ere .. 4140 
 . Lithia ane AC AC ... Trace 
 
 “This, however, must not be considered as conclusive, as it was made of a small 
 quantity, quite insufficient for the purpose; it will be seen that Mr. Staiger does not 
 even mention the carbonates of soda and magnesia which the water is known to contain 
 —in fact, in one hundred parts of solids the carbonate of soda constitutes 12'8.t 
 
 “There appear to be at present two main outlets for the water at (#) and (y), 
 while in two small holes hot water is met with, but overflows very feebly. The outlet 
 (a) in the sandy bed of the creek, about nine feet from the eastern bank, is connected 
 by piping with (vy), which is about twenty feet further east. The outlet (#) has an 
 elevation of from a foot to eighteen inches above the bed of the creek. 
 
 “Where the water emerges through the sand which fills the bed of the creek, a 
 square tub has been inserted in the sand to collect it. The water overflows, and a good 
 deal of it runs away down the creek. 
 
 
 
 * Australian Medical Gazette, January, 1891, p. 104. 
 + Brisbane: by Authority: 1891. 
 { L. Bruck, loc. cit. 
 
631 
 
 “A fairly large quantity of gas, which has a slightly sulphurous odour, is 
 constantly being given off with the water. 
 
 “ For some distance round the orifice (x), the sand still retains a considerable 
 portion of the heat derived from the percolation of the heated water through it. In 
 some places it is nearly impossible to place one’s hand in a hole dug in the sand to a 
 depth of about eight inches. A considerable portion of the water from the main 
 orifice still finds its way down the creek, by percolation through the sand without even 
 rising to the surface, 
 
 “No deposit exists around the mouth, but many of the pebbles in the more 
 immediate vicinity of the overflow are covered with an exceedingly thin white coating. 
 
 “The outlet (y) is on the bank of the creek, and a fair quantity of water rises 
 and is allowed to overflow into (x), but no gas appears to be emitted from this outlet. 
 
 “The pool (z) is distant about twenty feet south of (y). It is about three feet 
 by two feet across, and about ten to twelve inches deep. The temperature of the 
 water is much below that of the other two sources, and the quantity of overflowing 
 water is not nearly so great. The bottom of the pool is covered with a fine mud. 
 Bubbles of gas rise almost continuously through the water. 
 
 “About thirty feet further south, on the bank of the creek, another pool similar 
 to the last occurs. The water has a temperature slightly exceeding that of the 
 surrounding air. Very little water overflows, and no gas is emitted.’’ 
 
 Mitchell River Mud Springs.—In his Paper already quoted, Mr. E. Palmer 
 mentions some springs, with similar characteristics to those on the Flinders, as occurring 
 “about ten miles north of Gamboola Station, on the Mitchell River, with Pandanus 
 growing very plentifully through them,” and gives the following Analysis by Mr. Robert 
 Mar, Government Analyst, of “ a rather earthy sample of the saline incrustation”” from 
 these springs :— 
 
 Per cent. 
 “ Soda... aoe eee ooo vee doe eee eee eee 87°54 
 Lime... ene A00 Sr 5 was aes 50 cee ree eins; 
 Oxide of iron ee tes eA vee oa wae o bas Fal 
 Sand... we nee so BROT: 
 
 “‘ The acids are undetermined, but carbonic acid is chiefly represented. The water 
 of the springs is alkaline carbonated.” 
 
 Inniskillen Hot Springs—Mr. E. Palmer, in his Paper on “ Hot Springs and 
 Mud Eruptions,” already quoted, refers to “some small ones” on the Barcoo, below 
 Inniskillen (between Tambo and Blackall). 
 
 Between Langlo Downs and Whitechapel Creek (approx. Lat. 25° 30'S. and Long. 
 145° 50’ E.), I am informed by Mr. G. Neville Griffiths, several ‘extinct’? mud springs 
 have left mounds measuring about thirty feet in diameter at the base and about thirteen 
 feet in height. 
 
 Angy Springs, near Boulia, Lat. 22° 55'S., Long. 140° 25’ E.—I am also informed 
 by Mr. Griffiths that at Angy, about twenty-seven miles east of Boulia, between 
 Warrenda Creek and the Hamilton River, twenty or thirty strong springs are met with, 
 forming large mounds of white soda. The water is clear and of normal temperature. 
 
 Thargomindah Hot Springs—Hot mud springs are known to occur in the 
 neighbourhood of Thargomindah, but I am unable to give any description of them. In 
 a letter addressed to me on 24th September, 1889, the late Mr. C. S. Wilkinson 
 referred to a ridge of granite and gneiss, standing island-like in the Cretaceous 
 area, and added :—‘* This ridge lies chiefly on your side of the border, and is surrounded 
 with mud springs, one of which is a thermal spring. Probably the water is coming up 
 along the line of junction of the granite and Cretaceous beds.” 
 
632 
 
 South Australia.—To the above there may be added a short description of the 
 South Australian Mound Springs by Mr. H. Y. L. Brown * :— 
 
 ‘“‘The mound springs, which are the natural indicators of artesian water beneath 
 these plains,t are found in many places near the outcrops of bed rock,f between 
 the junction of which and the Cretaceous rocks the water has doubtless found an 
 easier egress. On the surface, the water often forms accumulations of travertine 
 limestone rising to heights of forty or fifty feet, and showing in the distance 
 across the level plains, where there is a group of springs, like a low range of hills; 
 the deposition of this limestone has in many instances formed raised cups or basins, 
 over the edges of which the water flows. The water of these springs contains soda, 
 and is generally good drinking water ; in some cases, however, in the same group of 
 springs, there is a great difference in the quality of the water, which in one spring may 
 be drinkable, and in another, a few feet away, salt. As a rule, these spring waters are 
 warm, and must have a considerable temperature beneath the surface.” 
 
 LIFE OF THE POST-TERTIARY AND RECENT PERIODS. 
 
 The following is the List, as revised by my Colleague, of extinct animals of whose 
 existence in Queensland since the close of Tertiary times we have direct evidence. The 
 names of such living animals as are associated with the extinct, in the same deposits, 
 are also given. It is, however, not within the scope of this work to publish a Census of 
 the present Fauna and Flora of the Colony. 
 
 The completeness of the break between the life of this Period and that of the 
 older Cretaceous Period is the first circumstance to strike an observer. The absence of 
 Tertiary organisms is equally noteworthy. The leading feature of the Fauna is the 
 immense development of some forms of life which at present distinguish the fauna of 
 Australia from all others, but which latter, after all, prove to be only a remnant of the 
 peculiar assemblage of animals that flourished in the same area in Post-Tertiary times. 
 Kangaroos, Wombats, Wallaroos, and other Marsupials were represented by a large 
 number of species now extinct, and the Wingless Birds were in greater numbers than in 
 the present day. 
 
 DIPROTODON BRECCIA, MARYVALH. 
 Class—PELECYPODA. 
 
 Order—VENERACEA. 
 Corbicula nepeanensis, Lesson Er ads or tes i ... Freshwater, Living 
 
 : Class—GASTEROPODA. 
 Order—PECTINIBRANCHIATA. 
 Melania onea, Adams and Angas san as ues ves AAO rr 
 »  balonensis, Conrad eis sae ae x 360 ee 7 
 »  denisoniensis, Brot aa fac 0b ae 5G aes 7 
 
 Order—PULMONATA. 
 Limnea rimosa? Adams and Angas ot ee sat a ves ” 
 
 Physa truncata, H. Adams... an nae ae Mr wae eae fA 
 
 Class—REpPTILIA. 
 
 Order—Crocopizia. 
 Crocodilus porosus, Schneider ce re me site ahs ons ms 
 
 * The Mesozoic Plains of South Australia. Proc, Austr. Assoc. Adv. Sct., 1889, i., p. 243. 
 
 + The Rolling Downs. 
 
 ~ Mr. Brown evidently means by ‘‘bed rock” the Paleozoic and Plutonic rocks underlying the 
 Cretaceous. 
 
633 
 
 Class—MAM™MALtA. 
 Order—MARsvUPIALIA. 
 Diprotodon australis, Owen 
 Macropus Titan, Owen 
 
 DARLING DOWNS. 
 Class—GASTEROPODA. 
 
 Order—PECTINIBRANCHIATA, 
 Melania balonensis, Conrad 
 
 Class—PIscEs. 
 
 Order—Dipno1. 
 Ceratodus Fosteri, Krefft 
 
 Class—-REPTILIA. 
 Order—CHELONIA. 
 Meiolania Oweni, Smith Woodward 
 Chelodina longicollis, Shaw 
 
 Order—LaAcERTILIA. 
 Chlamydosaurus Bennettii, Owen ... 
 Megalania prisca, Owen 
 Varanus dirus, De Vis 
 » emeritus, De Vis 
 Notiosaurus dentatus, Owen ? 
 
 Order—CrocopDIiLia. 
 Crocodilus porosus, Schneider : 
 
 Pallimnarchus pollens, De Vis __... we Soe 
 
 Class—-AVEs. 
 Order—CaRINATH. 
 Taphetus brachialis, Ne Vis 
 Necrastur alacer, De Vis 
 Pelicanus preavus, De Vis 
 Paleopelargus nobilis, De Vis 
 
 Platalea subtenuis, De Vis ... an a) ca ae ae as 
 Anas elapsa, De Vis es we ee a en ae 00 
 Dendrocygna validipinnis, De Vis ... in ae Ye ie ams 
 
 Biziura exhumata, De Vis ... 
 Nyroca reclusa,De Vis... 
 » robusta, De Vis 
 Plotus parvus, De Vis 
 LTithophaps ulnaris, De Vis... 
 Progura gallinacea, De Vis a ites a 500 ove ED 
 Chosornis preteritus, De Vis 
 Porphyrio? reperta, De Vis 
 
 os Mackintoshii, De Vis... nite ae aoe sr = 
 Gallinula strenuipes, De Vis 6 bei aes ts 
 7” peralata, De Vis =e pbc xo — Res 
 Tritonyx effluxus, De Vis ... one 
 
 Fulica prior, De Vis 
 Xenorhynchus nanus, De Vis 
 
 Order—RatiTZ. 
 Dromaius patricius, De Vis 
 
 “a gracilipes, De Vis ts Bod 
 Dinornis queenslandia, De Vis__... an 
 Metapteryx bifrons, De Vis Bt ar 
 
 Chosornis preteritus, De Vis noe on eee ee 07 Ks 
 
 Extinct 
 
 ”» 
 
 Extinct 
 Living 
 
 Extinct 
 
 Living 
 Extinct 
 
Echidna Owenii, Krefft ... 
 
 Ornithorhynchus agilis, De Vis 
 
 Phascolomys medius, Owen... 
 
 3 magnus, Owen 
 
 ry Mitchelli, Owen 
 
 oF parvus, Owen 
 
 ae platyrhinus, Owen 
 
 Thomsoni, Owen 
 
 33 
 Phascolonus gigas, Owen ... 
 Sceparnodon Ramsayi, Owen 
 Nototherium Mitchelli, Owen 
 
 , inerme, Owen ... 
 a dunense, De Vis 
 Diprotodon australis, Owen 
 . minor, Huxley 
 Euoenia grata, De Vis ie 
 robusta, De Vis 
 
 Phalanger procuscus, De Vis 
 
 Pseudochirus ? notabilis, De Vis 
 
 Koalemus ingens, De Vis_ ... 
 Archizonurus securus, De Vis 
 Thylacoleo carnifex, Owen... 
 Macropus Titan, Owen 
 
 3 affinis, Owen 
 
 A Ajax, Owen sis 
 * robustus, Gould ... 
 + sp. ind. (a) ye. 
 » ” (2) sige 
 
 Leptosiagon gracilis, Owen... 
 Osphranter Cooperi, Owen ... 
 Rs Gouldii, Owen ... 
 Palorchestes Azael, Owen ... 
 Pachysiagon Ferragus, Owen 
 ; Otuel, Owen ... 
 Phascolagus alétus, Owen 
 Procoptodon pusio, Owen ... 
 
 * Goliah, Owen... 
 - Rapha, Owen ... 
 Protemnodon Anak, Owen ... 
 - Anteus, Owen 
 % Mimas, Owen 
 Og, Owen 
 5s rechus, Owen... 
 Sthenurus Atlas, Owen 5 
 ¥ Brehus, Owen ... 
 
 Sthenomerus Charon, De Vis 
 Brachalletes Palmeri, De Vis 
 Triclis oscillans, De Vis 
 Synaptodon evorum, De Vis 
 Thylacinus speleus, Owen ... 
 Sarcophilus laniarius, Owen 
 ‘ prior, De Vis ... 
 Dasyurus viverrinus, Shaw ... 
 
 angustidens, De Vis 
 
 see 
 
 634 
 
 Class—MAMMALIA. 
 Order-—MoNOTREMATA. 
 
 Order—MARSUPIALIA. 
 
 Extinct 
 
 » 
 
 ” 
 Living 
 Extinct 
 
 ” 
 
 ” 
 
 ” 
 
 ” 
 
 ”» 
 » 
 » 
 
 ”» 
 
 ” 
 »” 
 ” 
 ”» 
 ”» 
 ” 
 
 ” 
 
 ” 
 
 ”» 
 ” 
 ” 
 ” 
 ”» 
 ”» 
 » 
 
 ” 
 
 » 
 ” 
 
 »” 
 Living 
 
635 
 
 Order—SIReEnra. 
 Chronozoon australe, De Vis Le nA a ea ee ... Extinct 
 
 Order—UnaGuuatTa. 
 Procherus celer, De Vis a aa 
 
 Order—PROBOSCIDEA. 
 Notoelephas australis, Owen ? ee aes wae aoe ee aks “A 
 
 EIGHT-M1ILE PLAINS, NEAR BRISBANE. 
 Class—PIsczs. 
 Order—DIpnot. 
 Ceratodus Fosteri, Krefft ... a Spi ee “2 ae ... Living 
 
 Class—R&Prinia. 
 Order—CrocopiLia. 
 Pallimnarchus pollens, De Vis__... aes ae ase oa a ” 
 
 CAIWAIROO, NEAR THARGOMINDAH. 
 Class—AVuS. 
 Order—RatitH. 
 Dromornis australis, Owen... fe sol e Sees ae ... Extinct 
 Dromaius patricius, De Vis abe cee, oa 56 aoe aa ay 
 
 PEAK DOWNS. 
 Class—AVES. 
 Order—RatTITz. 
 Dromornis australis, Owen ... ies aie aA ees i ane 7 
 
 OLSEN’S AND JOHANNSEN’S CAVES, ROCKHAMPTON. 
 Class —GASTEROPODA. 
 Order—PULMONATA. 
 
 Helix Cunninghami, Gray ... ise owe S50 rise ae .. Land, Living 
 »  Lncei, Pfeiffer... es o. ss re ar te if + 
 »  Whartoni, Cox oa wee ort ae. BA an sic ny 
 » Larson, Cox ... ae aes ae ae 5x ae abe op 
 
 RAISED BEACH, NUDGEE. 
 Class—PELECYPODA. 
 Order—OsTRACEA. 
 
 Ostrea pes-tigris, Hanley oe ny nee . Living 
 Order—ARCACEA. 
 Anomalocardia trapezia, Deshayes. ae ee ae sae ni ” 
 Order—PECTINIBRANCHIATA. 
 Potamides ebininus, Bruguiére. ... Bhs ane ae oh das 3 
 Natica plumbea, Lamk. S3 awe Ane ae a HO Ane = 
 RAISED BEACH, TOWNSVILLE. 
 Class—CRUSTACEA. 
 Order—DrEcapopa. 
 Thalassina Emerii, Bell. ... Ms eh bee wr ane ... Mxtinct ? 
 
 POST-TERTIARY DRIFTS. 
 STANTHORPE TIN FIELD. 
 
 The Stanthorpe Stream Tin Mines, on the borders of New South Wales, lie on the 
 surface of a granitic tableland, at an average elevation of a little less than three thousand 
 feet above the sea. The heads of the streams are shallow and swampy. Where the 
 streams attain any magnitude they find it easy to wander among the soft decomposing 
 surface of the granite country. The Severn, therefore, and its tributaries, such as 
 Quartpot Creek, have exceedingly tortuous courses and deep alluvial deposits. 
 
636 
 
 By far the greater part of the stream tin is in fine grains of the size of a pin’s 
 head and under, and almost always reveals under the lens some trace of an original 
 erystalline condition. It contains a large proportion of the “ruby” and “amber” 
 varieties. Together with quartz granules, it forms, as a general rule, the matrix of a 
 coarse, imperfectly cemented conglomerate or gravel of quartz and granite pebbles. The 
 pebbles are often rather squared than rounded. They are not of a nature to retain 
 striations well, but the shape of some of them leads me strongly to suspect that their 
 attrition might, in the first instance, have been due to glacial action. The crystalline 
 fragments of felspar, which have frequently been carried into the wash along with the 
 quartz and tin-stone, have in most cases decomposed into a stiff kaolin, which sometimes 
 helps to keep the wash together. 
 
 The tin wash is for the most part confined to the layer of gravel or uncon- 
 solidated conglomerate lying directly on the bed-rock. This gravel is generally 
 overlaid by a varying thickness (up to twenty-five feet or more) of gritty sand, which 
 is occasionally interrupted by thin layers of gravel (with streaks of tin-stone) or of 
 clay. 
 
 After an examination of the alluvial workings (in 1882), I concluded that the 
 tin-stone, in its original matrix, must have been in the form of crystals, rarely of large 
 size. ‘The ore was probably concentrated by the weathering of its matrix—whether reef, 
 lode, or dyke—and of the encasing granite country during a long period of gentle 
 subaérial denudation, when the rains were never sufficiently heavy to remove the tin, or 
 even the larger quartz stones, from the hillsides where they were left by the decay of 
 their matrix. To this there apparently succeeded a limited period of heavy rainfall, or 
 possibly of snow whose melting produced a rush of water sufficiently strong to “sluice” 
 the general surface of the hill country, and to deposit its heavier materials (including 
 the tin-stone) in the upper reaches of the Severn and its tributaries, while carrying off 
 its finer particles to the plains of the south-west. To the now current period belong 
 the accumulation, under temperate conditions, of the existing surface-wash on the hill- 
 sides (moderately rich in tin ore), and the deposition of the sand (almost destitute of 
 tin ore) which overlies the tin wash in the streams. 
 
 Two distinct types of tin-bearing rocks are met within the district—quartz reefs 
 and igneous dykes. 
 
 The reefs are best developed in the ridges on the left bank of Quartpot Creek, 
 nearly opposite Sommerville’s Homestead. Here are the outcrops of at least seven reefs 
 or veins, four of which bear north-north-east, one north-east, and one east and west. 
 These reefs are of highly crystalline quartz (sometimes smoky), and all contain much 
 wolfram and moderate-sized crystals of tin ore, the latter almost always confined to 
 faces and joints. Such reefs are apparently the sources of some of the coarser stream 
 tin which is locally met with. 
 
 The dykes are composed of granular quartz, fine scaly lithia-mica, and small 
 crystals of tin-stone, and form a rock much resembling the stanniferous greisen of 
 Saxony. They seem to have been erupted in a molten condition (bringing up the tin oxide 
 with them) among fissures in the granite. The tin-stone bears, in some samples I have 
 seen, a proportion of five or ten per cent. to the general mass of the rock. Dykes of 
 this character are seen at various points in the Range on the Boundary of the Colony 
 between the heads of Kettle Swamp and Sugarloaf Creek. They run at varying angles 
 from north-north-east to east-north-east, coinciding in their direction with a system 
 of jointing which characterises the granite. The tin-ore crystals of the dykes are 
 precisely what, with a little attrition, would form the main mass of the stream tin of the 
 heads of the Severn. 
 
637 
 
 Notwithstanding the-richness of the alluvial deposits of Stanthorpe, no payable 
 tin lode has yet been found on the Queensland side of the border. 
 
 The Stanthorpe Tin Field has never been geologically mapped in detail, but the 
 exhaustive Report of Mr. T. W. Edgeworth David on the Vegetable Creek Tin Mining 
 District of New South Wales throws considerable light on the subject. Mr. David 
 classifies the starniferous deposits as follows :— 
 
 Deposits of Tin Ore. 
 
 
 
 Alluvial Stream Works. Plutonic Veins. 
 
 Recent and Pleistocene Tertiary 
 “ Shallow Leads.” “Deep Leads,” 
 mostly capped by lava. 
 
 YrerpD oF StantHorRPE Tin FIELD. 
 
 
 
 
 
 Year. How Figures Obtained. nye Eh Tin eag 
 1872 1,407 109,816 
 1873 8,938 606,184 
 1874. 5,702 358,550 
 1875 From Ann. Rep. Dep. Mines for 1885 ... 4,475 237,879 
 1876 4,315 187,201 
 1877 3,335 133,432 
 1878 2,849 88,366 
 1879 | Total in Queensland 2,877 tons, value 
 5 £120,391 ; less Herberton 1314 tons, value 
 as £5 O60" Mae eh ae os 2,'7454 115,131 
 z ~ [1880 | Total in Queensland 2,847 tons, value 
 = a £142,977; less Herberton 193} tons, value 
 S28 STA Mee hee g Sioa arene nr 2,6534 135,237 
 2 8 1881 | Total in Queensland 3,456 tons, value 
 a £193,699; less Herberton 1,1834 tons, 
 zs Peele: £47,840 5 geo uso pe eo 5s 2,272 146,359 
 | o | 1882 Total in Queensland 4,261 tons, value 
 re aE ‘ £269,904; less Herberton 1,810 tons, 
 = value l7 0.400" ee. Lerten, 2,451 197,504 
 1883 a 817 40,233 
 1884 see 934 41,096 
 1885 ie 503 25,150 
 1886 a 430 24,940 
 1887 ozs 356 22,072 
 1888 sie 414 26,910 
 1889 “Oe 310} 16,146 
 1890 ses 277 14,404 
 Totals... nee 45,185 2,526,610 
 
 —_— SS 
 
638 
 
 MOUNT SPURGEON TIN FIELD. 
 
 This field was discovered in 1886, and has not yet attained great importance. It 
 is situated among slates and schists of undetermined age, although it is more than 
 likely that they belong, like the Hodgkinson Gold Field, to the Gympie Formation. 
 Lodes are known to exist, but the only export as yet has been stream tin ore. The 
 “Annual Report of the Department of Mines” for 1888 gives the amount for 1887 as 
 60 tons, valued at £4,800; and for 1888, 370 tons, valued at £18,500. The “ Report” 
 for 1889 gives 180 tons, valued at £6,980, for the year. The Report for 1890 gives 
 34 tons, valued at £1,530. 
 
 PASCOE TIN FIELD, CAPE YORK PENINSULA. 
 
 Stream tin has recently been discovered near the mouth of the Pascoe, but the 
 value of the discovery has yet to be tested. The tin ore probably came from the 
 granite country of the Carron and Janet Ranges. 
 
 J. = 
 
639 
 
 CHAPTER XXXVII. 
 
 THE ORGANIC REMAINS OF THE POST-TERTIARY PERIOD. 
 
 We have seen that during the Cretace.us Period in Queeusland, vertebrate 
 remains were confined to those of Enaliosaurian and Chelonian Reptilia, and fragmentary 
 remains of Fish. From this time onward, the geological record, paleontologically 
 speaking, is a blank. No fossiliferous Tertiary beds have been discovered—certainly 
 none of a marineorigin. The ‘raised beaches” near Brisbane and Townsville, which my 
 Colleague* says ‘“ have been classed as Tertiary,’’+ are doubtless simply of Post-Tertiary 
 age; whilst the existence of the Tertiary plant-beds described by the Hon. A. C. Gregory 
 as met with on Darling Downs,t requires confirmation, notwithstanding the presence of 
 “woody seed-vessels (Conchotheca turgida).” But, of the forerunners of the present 
 Avi, Reptilian, and Mammalian Faune ample and wonderful evidence exists in the 
 remains of the extinct, and frequently colossal vertebrates met with in the Post-Tertiary 
 or Quaternary Fluviatile Drifts of Queensland. So little geological knowledge appears 
 to have been displayed in the collection of these fossils, as to render them useless to the 
 geologist, for any but the broadest stratigraphical generalisations. 
 
 The only important attempt at a detailed description of these drifts is by Mr. 
 Gregory, under the name of “ Older Alluvial or Fossil Drift,’ but further information, 
 with the view of an attempted classification of these fluviatile deposits, is very desirable. 
 
 On several occasions Mr. C. W. De Vis has hinted at his belief that some portion 
 at least of the so-called Post-Tertiary Fauna should be regarded as appertaining to an 
 older geological period—for instance, the Pliocene. I am not aware that Mr. De Vis 
 has fully enunciated his views, but, no doubt, very much can be said in support of his 
 suggestion. 
 
 The fresh-water Mollusca accompanying the ossiferous remains are all living 
 species, so far as we know, but sufficient attention has not been paid by collectors to 
 this important point. 
 
 DESCRIPTION OF THE SPECIES. 
 
 Kingdom—ANIMALIA. 
 Sub-kingdom—ANNULOSA. 
 Class—CRUSTACEA. 
 
 Order—DECAPODA. 
 Family—THALASSINID 2. 
 
 Genus—THALASSINA, Latreille, 1806. 
 (Gen. Crust. et Insect., i., p. 51.) 
 THatassina Emertt, Bell, Pl. 36, fig. 6. 
 
 Thalassina Emerit, Bell, Proc. Geol. Soc., 1844, iv., p. 360. 
 39 is Etheridge fil., Cat. Australian Foss., 1878, p. 197 ( for synonymy). 
 
 Obs. The original specimen was described simply as coming from “ New 
 Holland,” without any further indication of precise locality or horizon. Prof. Bell 
 found some difficulty in fixing upon valid distinguishing characters between this species 
 and the recent form Thalassina anomala, Herbst. (7. scorpioides). 
 
 * Handbook Queensland Geology, 1886, p. 78. 
 
 + They were’so described to me by the late Professor Denton, but from the first time I had an oppor- 
 tunity of seeing them I regarded them as comparatively recent ‘‘raised-beach” deposits. (R.L.J.) 
 
 + Report on the Geological Features of the South-eastern District of Queensland, p, 2. Brisbane: . 
 by Authority: 1879 
 
640 
 
 From the time of Prof. Bell’s description to the discovery of the specimen which 
 came into my Colleague’s hands, nothing else appears to have been added to the history of 
 this peculiar fossil.* The present example, of which only the abdominal somites and the 
 legs are preserved, is contained in a blue limestone nodule. The three first pairs of 
 legs are almost entirely preserved, especially the second pair, but of the fourth and fifth 
 only small portions remain. The whole of the thorax has been removed, leaving the six 
 abdominal somites turned under and adpressed against the remains of the legs. Neither 
 the original figure nor the present specimen shows any trace of the lateral or sub- 
 marginal ridges visible on the abdominal segments of the recent ZT. anomala. Ina letter 
 dated Townsville, May 27th, 1881, my Colleague says, speaking of the present fossil, 
 ‘The nodule of limestone was picked up here, but | can throw no light on where it came 
 from. J do not know of any limestone on the coast uearer than Temple Bay, and No. 6 
 Northumberland Island.’’+ 
 
 Loc. and Horizon. Beach at Townsville (. L. Jack)—Post-Tertiary or Recent? 
 
 Sub-Kingdom—MOLLUSCA. 
 Section—MOLLUSCA VERA. 
 Class—PELECYPODA. 
 
 Order—OSTRACEA. 
 Family—OSTREIDZ. 
 
 Genus—OSTREA, Linneus, 1758. 
 (Syst. Nat., Ed. x., p. 696.) 
 
 OsTRFA PES-TIGRIS, Hanley, Pi. 36, figs. 7-9. 
 
 Ostrea pes-tigris, Hanley, Proc. Zool. Soc., 1845, xiii., p. 106. 
 » mordax, Gould, Wilkes’ U.S. Explor. Exped., 1852, xii. (Mollusca and Shells), p. 464, Atlas, 
 f. 575, a and b. 
 
 Obs. Several examples of a small Oyster, still retaining traces of the deep red 
 purple colour characteristic of this species, as described by Gould, as well as the 
 spatulate outline and solid structure, have been collected from Post-Tertiary deposits by 
 my Colleague. The attached valve shows the “erect triangular tooth-like folds” for the 
 reception of the digitations of the larger valve; and also the concentrically-arranged 
 pits round the margin within the valve, together with the darkly-stained adductor-scar. 
 
 Authenticated specimens of Ostrea pes-tigris, Hanley, have been compared with 
 the present specimens, and also recent Australian shells, by Mr. EH. A. Smith and the 
 Writer, and we believe them to be identical. Hanley’s specimens were derived from 
 Borneo, Gould’s from Fiji, and, being identical, the former’s name must be adopted. 
 
 Dr. J. C. Cox, in his Paper, “ On the Edible Oysters found on the Australian 
 
 and Neighbouring Coasts,” says :—“ This species is a rock oyster found adhering very 
 firmly to the rocks by the whole of the lower valve, from Brisbane in Queensland to far 
 north beyond Port Denison . . . and probably all along the coast north of 
 
 Moreton Bay to Cape York, and at Lord Howe’s Island.’’} 
 Loe. and Horizon. Child’s Vineyard, Nudgee, about nine miles from Brisbane 
 (R L. Jack)—Estuarine Beds (Raised-beach). 
 
 * A number of specimens, apparently of the same species, were collected by the late Mr. James Smith, 
 shortly before his death, at Casuarina Island, Keppel Bay. They occur in limestone nodules, and are now in 
 the Geological Survey Collection, but have not yet been seen by my Colleague. (R.L.J.) 
 
 ++ These limestones are Palaozoic. (R.L.J.) 
 
 t Proc. Linn. Soc. N. S. Wales, 1883, vii., p. 130. 
 
641 
 
 Order—ARCACEA. 
 Family—ARCID 2. 
 
 Genus—ANOMALOCARDIA, Klein, 1758. 
 (Tentamen Meth. Ostracol.) 
 
 ANOMALOCARDIA TRAPEZIA, Deshayes, Pl. 36, figs. 10-12. 
 Arca trapezia, Deshayes, Mag. Zool. 
 3, lobata, Reeve, Conch. Icon. (Mon, Avca), 1844, ii., Sp. 19, t. 3, f. 19. 
 Anomalocardia trapezia, Angas, Proc. Zool. Soc., 1867, p. 931. 
 
 Sp. Char. Shell obliquely-rhomboid, much produced posteriorly, and post- 
 ventrally, gibbous and prominent in the umbonal region; test solid, inner margins 
 strongly toothed. Hinge-line shorter than the width of the shell-area, which is elongately 
 triangular, with two to four or five cartilage grooves, and transversely striate; teeth 
 about forty-five in full-grown specimens; umbonal region convex and gibbous, pro- 
 jecting upwards much above the hinge-line ; umbones anteally incurved. Anterior ends 
 small, the margins obliquely rounded, insensibly passing into the ventral, which is 
 similar; posterior sides variable in their proportions, sometimes abruptly sub-truncate, 
 at others becoming expanded and rather flattened, with an obliquely elevated hinge- 
 line, their margins rounded ventrally, and obliquely truncated more or less dorsally ; 
 muscular impressions strongly marked. Surface with numerous strong radiating ridges 
 or cost, quite two-thirds of which are inclined towards the posterior, and becoming 
 much flattened on the posterior slope, crossed by concentric frillings, and rising on the 
 cost into echinations. 
 
 Obs. Amongst an abundance of this species is a shortened and very gibbous 
 variety, with high elevated umbones, and greatly produced in a posterior ventral 
 direction (Pl. 36, figs. 11 and 12), and in which the marginal crenulations are also very 
 strong. 
 
 Reeve gives the locality of this common Australian shell wrong, as he does in so 
 many other cases—viz., the West Indies. The National Collection in London contains 
 numerous examples from the Brisbane Water, which entirely correspond with the fossil. 
 
 Loc. and Horizon. Child’s Vineyard, Nudgee, about nine miles from Brisbane 
 (R. L. Jack) — Estuarine Beds (Raised-beach). 
 
 Order—VENERACEA. 
 Family—CYRENIDZ. 
 
 Genus—CORBICULA, Megerle, 1811. 
 (Berlin. Magazin, 1811, p. 56.) 
 
 CoRBICULA NEPEANENSIS, Lesson. 
 
 Cyclas Nepeanensis, Lesson, Voy. Coquille, Zoologie, 1830, ii., p. 428, Atlas, t. 13, f. 14, g-n. 
 Cyrena Australis, Deshayes, Eacyclop. Method., 1830, Vers. ii., No. 12, p. 50. 
 Corbicula Australis, Deshayes, Cat. Conchif. Brit. Mus,, 1854, p. 230. 
 Daintree, Quart. Journ. Geol. Soc., 1872, xxviii., p. 274. 
 . “fA Smith, Journ. Linn. Soc. (Zool.), 1883, xvi., p. 300, t. 17, f. 26 and 27. 
 
 Obs. This is probably the shell cited by the late Mr. Richard Daintree as 
 occurring with Diprotodon remains at Maryvale Creek. The specimens of these 
 freshwater shells are not forthcoming now, which is to be regretted, because fresh 
 comparisons would have been advantageous. 
 
 Loc. and Horizon. Maryvale Creek, Clarke River, North Queensland (The late 
 R. Daintree) —Diprotodon-breccia, 
 
 28 
 
 9? ” 
 
642 
 
 Class—GASTEROPODA. 
 
 Order—PECTINIBRANCHIATA. 
 Family—MELANIID. 
 
 Genus—MELANIA, Lamarck, 1801. 
 (Syst. Anim. sans Vertéb., p. 91.) 
 
 Metania onca, A. Adams and Angas. 
 
 Melania onca, A. ieee and Angas, Proc. Zool. Soc., 1863, p. 415. 
 ap Brot, Kiister’s Conchyl. Cabinet, Edit. 2, 1874, p. 330, t. 34, f. 7. 
 ? 4,  arca, Daintree, Quart. Journ. Geol. Soc., 1872, xxviii., p. 274. 
 oF onca, Smith, Proc. Linn. Soe. (Zool.), 1888, xvi., p. 259. 
 
 Obs. The name Melania arca occurring in Mr. Daintree’s “Notes on the 
 Geology of the Colony of Queensland ” is probably a misprint for the above species. 
 
 Loc. and Horizon. Maryvale Creek, Clarke River, North Queensland (The late 
 Rk. Daintree) —Diprotodon-breccia. 
 
 MELANIA BALONENSIS, Conrad. 
 Melania Balonensis, Conrad, Prod. Acad. Nat. Sc. Philadelphia, 1850, v., p. 11. 
 
 = 7 Conrad, American Journ. Conchol., 1866, ii., p. 80, t. 1, f. 10. 
 55 " Brot, Kiister’s Conchyl. Cabinet, I., Edit. 2, 1874, p. 287, t. 28, f. 14, 14a and 0, and 15. 
 4 ty) Smith, Proc. Linn. Soc. (Zool.), 1883, xvi., p. 257, t. 5, f. 1-3. 
 
 », pagoda, Daintree (non Lea), Quart. Journ. Geol. Soc., 1872, xxviii., p. 274. 
 
 Obs. There appears to be much variation in size and appearance, both in the 
 living and fossil individuals of this species, especially in form and stoutness, whilst a 
 few of the fossils are more elongate than any of the recent examples in the British 
 Museum. The former certainly_ appears to have grown to a larger size than the latter. 
 This is probably the species recorded in Mr. Daintree’ s Paper as Melania pagoda, which 
 is not known as an Australian living species. 
 
 Loc. and Horizon. King’s Creek, Darling Downs, in Post-Tertiary deposits 
 associated with extinct marsupial remains (Dr. G. Bennett—Colln. British Museum) ; 
 Maryvale Creek, Clarke River (The late R. Daintree) —Diprotodon-breccia. 
 
 MELANIA DENISONIENSIS, Brot. 
 
 Melania Denisoniensis, Brot, Kiister’s Conchyl. Cabinet, Edit. 2, 1874, p. 234, t. 25, f. 6. 
 . - Smith, Journ. Linn. Soe. (Zool.), 1883, xvi., p. 259, t. 5, f. 4-8. 
 »,  mesta, Daintree (non Hinds), Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 274. 
 Obs. In all probability this is the species mentioned by Mr. Daintree as 
 Melania mesta. 
 Loc. and Horizon. Maryvale Creek, Clarke River, North Queensland (The late 
 R. Daintree)—Diprotodon-breccia. 
 
 Family—CERITHIID A. 
 Genus—POTAMIDES, Brongniart, 1822. 
 
 - (Descrip. Géol. Environs Paris.) 
 
 POTAMIDES EBININUS, Bruguiére, sp., Pl. 36, fig. 14-16. 
 
 Cerithium ebininum (Brug.), Deshayes, in Lamarck, Hist. Nat. Anim.s. Verttb., 2nd edit., 1843, ix., p. 287. 
 Potamides ebininus, Reeve, Conch. Icon. (Mon. Potamides), 1866, xv., Sp. 2, t., f. 2a, 2b, and 2. 
 
 Sp. Char. Shell elongately pyramidal; whorls twelve-fourteen, concave above, 
 convex below; body-whorl usually highly varicated ; sutures well marked; apex acute ; 
 angles of the whorls bearing a series of obtuse prominent tubercles, which fall into a 
 
643 
 
 series of obliquely vertical lines, the surface being otherwise spirally ridged, the ridges and 
 intervening sulci about equal, the former passing over the tubercles. Aperture much 
 expanded ; canal oblique, open and wide; outer lip very much foliated and thickened, 
 with a sinuosity of greater or less depth; inner lip reflected, thickened above and 
 beneath. 
 
 Obs. This fine species appears to occur in a fossil state near Brisbane in as great 
 profusion as it does in the estuaries of the eastern coast of Australia at the present 
 time. In some specimens the mouth is greatly thickened, especially the outer lip, 
 forming a strong varex (Pl. 36, fig. 16). Its amount of sinuosity also varies, being very 
 sharp in some specimens, and obtuse in others, when the lip is much thickened. 
 
 Loe. and Horizon. Child’s Vineyard, Nudgee, about nine miles from Brisbane 
 (R&. L. Jack)—HEstuarine Beds (Raised-beach). 
 
 Family—NATICIDA. 
 
 Genus—NATICA, Adanson, 1757. 
 (Hist. Nat. Sénégal, Coquil., p. 172.) 
 
 Natica pLuMBEA, Lamarck, Pl. 36, fig. 18. 
 Natica plumbea, Lamarck, Hist. Nat. Anim. sans Vertéb., 1822, vi., Pt. 2, p. 198. 
 Ap - Reeve, Conch. Icon. (Mon. Watica), 1855, ix., Sp. 34, t. 9, f. 34, a and b. 
 Obs. The fossil possesses the oblong-turbinate shape, conoid spire, infra-sutural 
 flattened space on each whorl, and the narrow, elongate umbilicus of Natica plumbea. 
 Loc. and Horizon. Child’s Vineyard, Nudgee, about nine miles from Brisbane 
 (2. L. Jack)—Estuarine Beds (Raised-beach). 
 
 Order—PULMONATA.* 
 
 Obs. We are greatly indebted to Mr. Charles Hedley, F.L.S., for the following 
 epitome of his views on the origin and distribution of the Australian Pulmonifera. As 
 these have an interesting geological bearing we are glad to avail ourselves of the 
 opportunity of inserting them + :— a 
 
 “One of the most remarkable facts yielded by an analysis of the Australian 
 Land Molluscan Fauna is that the operculate snails are confined to a narrow strip of 
 landalong the Queensland coast. Proceeding southwards from Torres Straits they diminish 
 gradually till the last outpost of the invading army is reached about the Clarence River, 
 in N.S. Wales. The sole apparent exception to this rule is Zrwncatella, which spreads 
 to Tasmania and South Australia, but as this genus is strictly littoral, and evidently 
 migrates not by land but by sea, it cannot be considered as a disturbing factor in my 
 generalisation. Contrasting the fauna of Queensland with the more typically Australian 
 and probably archaic fauna of Tasmania, Victoria, and Western Australia on the one 
 side, and that of New Guinea on the other, it will be seen that this foreign aspect of the 
 
 
 
 
 
 * In addition to the species enumerated here, Messrs. C, T. Musson and C. Hedley have recorded 
 the following species from Olsen’s Caves :— 
 Helix (Charopa) iuloidea, Forbes. 
 », (Rhytida) splendidula, Pf. 
 re Ap ae 5, var. strangeoides, Cox. 
 Pupina Coxi, Morelet. 
 »  meridionalis, PE. 
 (See Proc. Linn. Soc. N. 8. Wales, 1892, vi. (2), pp. 551-564.) 
 + Land Molluscan Fauna of British New Guinea (Anatomical Supplement). Proc, Linn. Soe. 
 NV. S. Wales, 1892, vi. (2), Pt. 4, p. 694, 
 
644: 
 
 operculate genera Pupina, Helicina, and Diplommatina is shared by the inoperculate 
 forms of Atopos, Hadra, Chloritis, and Papuina; A. prismaticus of Papua claiming 
 affinity with 4. australis of Queensland, H. Broadbenti with H. informis, C. chloritoides 
 with C. Porteri, and P. naso with P. Macgillivrayi. The species actually common to 
 both regions are few ; B. Macleayi inhabits both countries, ZT. annula only finds a place 
 in the Queensland catalogue by courtesy, while P. pedicula, S gracilis, T. ceylanica, 
 T. valida, and L. vitrewm are widespread throughout Polynesia. From these premises 
 it may be deduced that this portion of the Queensland molluscan fauna, though isolated 
 sufficiently long to have lost specific identity with that of Papua, has nevertheless been 
 derived from it. 
 
 “The shallow sea of Torres Straits now severs this Continent from the 
 adjoining Island. Were its bed raised but seven fathoms the two countries would be 
 united, while an elevation of ten fathoms would form a wide bridge between them. 
 When the marine life east and west of Torres Straits is better known it will be of 
 interest to observe whether the influence of an ancient isthmus is still visible in any 
 divergence between the fauna inhabiting the two areas. 
 
 “ Further to the westward the coasts of Australia and New Guinea again converge, 
 being separated by an arm of the Arafura Sea, which gradually shoals from a central 
 depth of forty fathoms, and stretches for about a hundred and fifty miles between Cape 
 Wessel in the Northern Territory, and Cape Valsche on the opposite shore of Dutch 
 New Guinea. 
 
 “In the ‘Transactions of the Royal Society of S. Australia’ (vol. v., 
 pp. 47-56), Professor Tate enumerates the Land and Freshwater Mollusca of 
 tropical S. Australia. It is remarkable that whereas a third of the land shells of 
 Papua, and a sixth of the land shells of Queensland, are operculate, his census 
 includes no operculate land shells whatever. Thus, at the remote date when the 
 ancestors of the present Queensland molluscan fauna migrated from New Guinea 
 across the ancient isthmus that I suppose to have bridged Torres Straits, the 
 Arafura Sea appears to have still presented an impenetrable barrier between the two 
 countries. The former elevation of land in this region, if uniform from east to west, 
 may therefore be calculated at more than seven and less than forty fathoms.” 
 
 Family—LIMN IDA. 
 
 Genus—LIMN AIA, Lamarck, 1799. 
 (Prodrome—Mém. Soc. Hist. Nat. Paris, 1799.) 
 Amphipeplea vinosa, A. Adams and Angas, Proc. Zool. Soc., 1863, p. 415. 
 Limnea (Amphipeplea ?) vinosa, Smith, Journ. Linn. Soc. (Zool.), 1883, xvi., p. 273. 
 35 rimosa, Daintree, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 274. 
 
 Obs. The name Limnea rimosa, given in Mr. Daintree’s Paper, probably refers 
 to this species. 
 
 Loc. and Horizon. Maryvale Creek, Clarke River, North Queensland (The 
 late R. Daintree)—Diprotodon-breccia. 
 
 Genus—PHYSA, Draparnaud, 1801. 
 (Tab. Moll. Terr. Fluy. France.) 
 
 Puysa truNcaTA, H Adams. 
 
 Physa (Ameria) truncata, H. Adams, Proc. Zool. Soc., 1861, p. 144. 
 » truncata, Daintree, Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 274. 
 3, (Ameria) truncata, Smith, Journ. Linn. Soc. (Zool.), 1883, xvi., p. 292. 
 
 Loc. and Horizon. Maryvale Creek, Clarke River, North Queensland (The late 
 . Daintree)—Diprotodon-breccia,. 
 
645 
 Family—HELICID A. 
 
 Genus—HELTIX, Linnéus, 1758. 
 (Syst. Nat., Ed., x. 
 
 Herrx (Pepryoeyra) CuNNINGHAMI, Gray. 
 
 Helix Cunninghami, Gray, Proc. Zool. Soc., 1834, p. 64. 
 +3 + Reeve, Conch. Icon. (Mon. Helix), 1852, vii., t. 7, f. 363. 
 .5 Cox, Mon. Australian Land Shells, 1868, p. 52, t. 1, f. 5 and 5a. 
 of (Padincgura) Cunninghami, Pilsbury in Tryon, Man. Conch., 2d. Ser., vi., Helicide, iv., Pt. 21, 1890, 
 p. 14, t. 2, f. 28-31. 
 
 Obs. A very large and remarkable shell, of which a much decorticated example 
 was obtained by the late Mr. James Smith. It is now living around Port Curtis and 
 Rockhampton. It is a depressed discoid, and very solid shell, with a scarcely pro- 
 minent spire; four or five quickly-increasing whorls, the last being very wide and bluntly- 
 keeled, and suddenly deflected in front.. The umbilicus is very large and open, so as to 
 form what Mr. U. Reeve calls “a wide perspective basin,’ this being one of the chief 
 characters of the shell. The fossil has a diameter of three and three-quarter inches. 
 
 Loc. Olsen’s Cave, Rockhampton, in red stalagmitic limestone (Lhe late James 
 Smith). 
 
 Hetix (Hapra) Incer, Pfeiffer. 
 Helix Incei, Pfeiffer, Proc. Zool. Soc., 1845, p. 126. 
 3 », Reeve, Conch. Icon. (Mon. Helix), 1852, vii. t. 68, f. 356, a-c. 
 ss »» Cox, Mon. Australian Land Shells, 1868, p. 54, t..5, t. 18, f. 1. 
 »,  (Hadra) Incei, Pilsbury, in Tryon, Man. Conch., 2nd. Ser., vi., Helicide, iv., Pt. 21, 1890, p. 167, 
 t. 39, f. 77-81. 
 
 Obs. The sub-fossil form very closely resembles the figures of Reeve. It is a 
 depressed-globose umbilicated shell, with a convexly-conoid spire; whorls are six in 
 number, the last large and well-rounded, and the columellar margin reflected and 
 nearly covering the umbilicus. The shell is finely preserved and encrusted with 
 stalagmite. 
 
 Loc. and Horizon. Johannsen’s Cave, Rockhampton, in stalagmite (Zhe late 
 James Smith). 
 Heurx (Hapra) Wuartont, Cox. 
 Helix Whartoni, Cox. Proc. Zool. Soc., 1871, p. 55, t. 3, f. 5, 5a. 
 »  (Hadra) Whartoni, Pilsbury in Tryon, Man. Conch., 2nd. Ser., Helicide, iv., Pt. 21, 1890, p. 171, 
 t. 19, f. 31, 32, t. 33, f. 68, 69. 
 
 Obs. This is an openly umbilicate, depressed-globose thin shell, with a rather 
 raised spire; there are six and a-half flattened whorls, the last descending in front. 
 The columellar margin of the aperture is triangular and dilated, half concealing the 
 umbilicus. H. Whartoni is found around Port Denison. The shell is finely preserved 
 in the fossil. 
 
 Loc. Johannsen’s Cave, Rockhampton, in stalagmite (Zhe late James Smith). 
 
 Herix (Hapra) Parsont, Coz. 
 
 Helix Parsoni, Cox, Proc. Zool. Soc., 1872, p. 18, t. 4, f. 2. 
 
 », (Hadra) Parsoni, Pilsbury in Tryon, Man, Conch., 2nd Ser., vi., Helicide, iv., Pt. 21, 1890, p. 162, 
 t. 80, £. 11-13; 
 
 Obs. H. Parsoni is described by Dr. Cox as a globose-conical shell, with an 
 obtusely conical round spire, and a deep open umbilicus; whorls seven, convex; the 
 suture margined with a distinct white line; the last whorl produced and deflected in 
 front, and the base flattened. The aperture is ovately lunar, with a slightly thickened 
 
646 
 
 peristome, expanded and reflected throughout; the collumellar margin triangularly 
 dilated, and overhanging the large umbilicus. The specimen is a decorticated example. 
 Loc. Olsen’s Cave, Rockhampton, in red stalagmitic limestone (Zhe late James 
 Smith). 
 Genus—BULIMUS, Scopoli, 1777. 
 (Introd. Hist. Nat.) 
 
 Section—PLACOSTYLUS, Beck, 1837. 
 (Index Moll., p. 57.) 
 
 Buiimus (PLAcOsTYLUS) FIBRATUS, Martyn. 
 
 Limasx fibratus, Martyn, Univ. Conch., 1734, t. 25. 
 Bulimus fibratus, Gray in Diffenbach, Travels in New Zealand, 1848, ii., p. 247. 
 »,  Bairdii, Reeve, Conch. Icon. (Mon. Bulimus), 1848, v., t. 48, f. 272. ‘ 
 
 Obs. A specimen of this species, with a portion of the body-whorl wanting, was 
 presented to the British Museum by the late Mr. R. Daintree, and was said to have 
 been collected in “ Australia.” The section Placostylus has not hitherto been observed on 
 the Australian Continent, although known from many of the Pacific Islands, and the fossil 
 must therefore remain doubtfully associated with its former fauna. An error may 
 have been committed, but as Mr. Daintree was known to be a careful collector and keen 
 observer, the species is provisionally included amongst the latter. The specimen retains 
 the coarsely rugate appearance of B. fibratus, and is preserved in a fine ochre-yellow 
 sandy matrix. 
 
 Sub-kingdom—VERTEBRATA. 
 Class—PIScES. 
 Order—DIPNOI. 
 Family—LEPIDOSIRENIDA. 
 
 Genus—CERATODUS, Agassiz, 1838. 
 (Poissons Foss., iii., pp. 129 and 166.) 
 
 Crratopus Forstert, Krefft. 
 
 Ceratodus Forsteri, Krefft, Proc. Zool. Soc., 1870, p. 221, p. 222, f. 1-3. 
 5 a Gunther, Phil. Trans., 1872, clxi., Pt. 2, pp. 511 and 514, t. 30, f. 2 and 3, t. 31, f. 1-9, 
 t. 32, f. 1 and 2, t. 33, f. 1-3, t. 34, f. 1-3, ete. 
 3 Palmeri, Krefft, Nature, 1874, ix., p. 293. 
 _ Forstert, Huxley, Proc. Zool. Soc., 1876, p. 24. 
 Pf “s De Vis, Proc. R. Soc. Queensland, 1884, i., Pt. 1, p. 40. 
 Ff Fs Smith Woodward, Cat. Foss. Fishes Brit. Mus., Pt. 2, 1891, p. 274. 
 
 Obs. The late Mr. Gerard Krefft appears to have been the first to call attention 
 to the fossil remains of this very remarkable genus. In a short communication 
 forwarded to “‘ Nature”’ he recorded the discovery of the left upper dental plate of a 
 Ceratodus, to which he applied the name C. Palmeri, on the grounds that the tooth 
 was larger than the corresponding one in C. Forsteri, the enamel coarser, and the surface 
 more undulated. 
 
 The single tooth acquired by Mr. Krefft has since been supplemented by others 
 obtained for the Queensland Museum, consisting of four pterygopalatine plates and 
 five mandibulary. Of these teeth Mr. De Vis states—“ We can perceive an approximate 
 similarity in their leading features, which enables us to avoid the error of considering 
 them all of different species, and leads us to regard them as not only one, but one with 
 the living C. Forsteri.”’ 
 
647 
 
 Loc. and Horizon. Darling Downs (C0. W. De Vis, Colln. Queensland Museum)— 
 Chinchilla Conglomerate. A Ceratodus tooth has also been obtained at the depth of 
 about seventy feet from a well sunk in the Eight-mile Plains, near Brisbane. 
 
 Class—REPTILIA. 
 
 Order—CHELONTIA. 
 Family—MEIOLANIIDA.* 
 
 Genus—MBEIOLANTIA, Owen, 1886. 
 (Proc. R. Soe., xl., p. 315.) 
 
 Meronanta Owent, Smith Woodward. 
 Megalania prisca, Owen, Phil. Trans. 1881, clxxi., Pt. 3, p. 1087, t. 37, f. 1, t. 38; £. 1-3. 
 an Owen, Loe, cit., elxxii., Pt, 2, p. 547, t. 64, t. 65, f. 1-4. 
 Ceiichet ys sthenurus, Huxley, Bree. R. Soc.; 1887, xliii., p. 237 (Queensland cranium and tail-sheath). 
 Meiolania Oweni, Smith Woodward, Ann. il Mag. Nat. Hist. 1888, i., p. 89. 
 Miolania Oweni, Lydekker, Cat. Foss. Reptilia and Amphibia Brit. Mus., Pt. 3, 1889, p. 166. 
 
 Obs. A few pages further on will be explained the restriction which has been 
 made in the use of the name Megalania prisca, Owen. It appears that it originally 
 included—(aq), lacertilian vertebre, and an occipital fragment; (6), a chelonian skull 
 and tail-sheath ; and (c), marsupial foot-bones. ‘The name is now restricted to the first 
 of these, the chelonian skull and tail-sheath being referable to Owen’s later described 
 genus Mevolania. 
 
 This skull, found by Mr. G. I’. Bennett in 1871, at King’s Creek, Darling Downs, 
 was spoken of by Sir Richard Owen as that of a Lacertilian, in the following words—‘ They 
 [z.e., the pieces] included unquestionable horn-cores, and the fore-part of an upper 
 jaw, showing no trace of teeth or sockets on the alveolar border. . . . . . . On 
 restoring the cranium, as far as its transmitted fragments could be correctly juxtaposed, 
 it manifested, in one part, not only a well-defined surface from which an apparently 
 autogenous horn-core, as in the Giraffe, had become detached, but also pairs of exogenous 
 ones like those of the Ox. The longest of these extended from the upper and side 
 borders of the hinder portion of the cranial specimens, but evidently anterior, as in the 
 Bison, to the occipital ridge. The surface, seemingly for the sutural attachment of a 
 horn-core, was on the upper part of the nasal bone, symmetrical in shape, crossing 
 the mid-line, like the horn of a Rhinoceros.’’ Only in the small Australian Lizard— 
 Moloch horridus, Gray—could Owen find a head ‘resembling in its proportionate 
 breadth and shortness that of Megalania.” 
 
 The tail-sheath was found in 1881, at the same spot as the previous specimen, and 
 was referred by Owen to the same animal. The specimen included three annular 
 segments, and the terminal cap of an osseous sheath. ‘ Each of the annular segments,” 
 says Prof. Owen, “sends off two pairs of massive conical processes, like the horn-cores 
 of the skull, but of a larger size. This caudal armour resembles that seen in Uromastia 
 princeps, O’Shaugn., from Zanzibar, and more particularly still that of Moloch horridus, 
 Gray.” These remains were obtained by Mr. G. F. Bennett at King’s Creek, Darling 
 Downs. 
 
 The researches of Prof. Huxley + on other similar remains from Lord Howe 
 Island, named Metolania platyceps and M. minor by Prof. Owen,t{ and having the greatest 
 
 * Boulenger, Proc. Zool. Soc. 1887, Pt. 3, p. 554; Gunther, Encyclop. Brit., 9th Edit., 1888, xxiii., 
 p. 457, 
 
 + Proc, R. Soc., 1887, xliii., p. 237. 
 t Phil. Trans., 1886, clxxvii., Pt, 2, p. 471, t. 29-31. 
 
648 
 
 possible resemblance to the skull from King’s Creek, but smaller in size, appear to put 
 it beyond doubt that these fossils are Chelonian and not Lacertilian. They are believed 
 to be most nearly allied to Ohelydra and Gypochelys, Cryptodiran genera. A full 
 explanation of this matter will be found a few pages further on. 
 
 The occurrence of this genus of Chelonia in Queensland is exceedingly interest- 
 ing, because the section of the order to which it appertains is not otherwise represented 
 in Australia. This statement of Prof. Huxley’s has been controverted by Mr. G. A. 
 Boulenger,* who considers that Meiolania is a member of the group to which the 
 Australian forms belong—viz., the Pleurodira. The balance of evidence, however, 
 favours Prof. Huxley’s view.t In concluding a brief review of this subject Mr. R. 
 Lydekker makes the following pertinent remarks {:—‘ Perhaps the acquisition of the 
 plastron may be necessary before we can be absolutely certain as to the Pleurodiran 
 nature of Miolania, but in the first place distributional evidence is very strongly in 
 favour of this view, while the osteological evidence adduced by Boulenger seems still 
 more so. That the genus represents a distinct family there can be no question whatever. 
 
 Loc. and Horizon. King’s Creek, Darling Downs (G. F. Bennett—Colln. Brit. 
 Mus.)—Fluviatile deposits. 
 
 Family—CHELYID&. 
 
 Genus—CHELODINA, Fitzinger, 1826. 
 (N. Class Rept., p. 6.)§ 
 
 CHELODINA LONGICOLLIS, Shaw. 
 
 Testudo longicollis, Shaw, Gen. Zool., 1802, iii., p. 62, t. 16. 
 Chelodina longicollis, Gray, Syn. Rept., 1831, p. 39. 
 ” a Lydekker, Cat. Foss. Reptilia and Amphibia Brit. Mus., 1889, Pt. 3, p. 168. 
 
 Obs. The British Museum Collection contains an imperfect nuchal bone, a 
 tenth marginal bone of the right side, and a small right humerus, said to be of this 
 species. : 
 Loc. and Horizon. Westbrook, branch of Oakey Creek, Condamine River (Dr. 
 G@. Bennett—Colln. Brit. Mus.)—Fluviatile deposits. 
 
 Order—LACERTILIA. 
 Family—AGAMID&. 
 
 Genus—CHLAMYDOSAURUS, J. H. Gray, 1827. 
 (P. P. King’s Survey, Coasts of Australia, ii., p. 424.) 
 
 CHLAMYDOSAURUS BENNETTII, Owen, m.s. 
 
 Chlamydosaurus Bennettiit, Owen in Bennett, Papers and Proc. R. Soc. Tas. for 1875 [1876], p. 57. 
 
 * Kingi, Lydekker (non Gray), Cat. Foss. Reptilia and Amphibia Brit. Mus., Pt. 1, 1888, p. 276. 
 
 Obs. The Frilled Lizard (C Kingii, Gray), appears to be represented in the 
 Quaternary Deposits of Queensland by an extinct species which has received the ms. 
 name of C. Bennettiz, Owen. 
 
 The remains, consisting of part of ajaw with teeth, were found by Mr. G. F. 
 Bennett, and forwarded to Prof. Sir R. Owen, but the fragment has never been 
 
 * Proc. Zool. Soc., 1887, Pt. 3, p. 554; Ann. and Mag. Nat. Hist., 1889, iii., p. 188. 
 + See Bauer, Ann. and Mag. Nat. Hist., 1889, iii., p. 54. 
 
 + Cat. Foss. Reptilia and Amphibia Brit. Mus., Pt. 3, 1889, p. 160. 
 
 § Fide Lydekker, Cat. Foss. Reptilia and Amphibia Brit. Mus., Pt. 3, 1889, p. 168. 
 
649 
 
 described in detail. The extinct species differs from its living representative, Dr. G. 
 Bennett says, by possessing a shorter, more obtuse, and higher head. On the other 
 hand, Mr. R. Lydekker states that it does not show any characters by which it can be 
 distinguished from the living species. 
 Loc and Horizon. Gowrie Station, Darling Downs (G. F. Bennett)—Fluviatile 
 deposits. 
 Family—VARANIDZ. 
 
 Genus—MEGALANTA, Owen, 1858.” 
 (Proc. R. Soc., ix., p. 273.) 
 
 MEGALANIA PRISCA, Owen. 
 
 Megalania prisca, Owen, Proc. R. Soc., 1858, ix., p. 273. 
 » Owen, Phil. Trans., 1860, cxlix., p. 43, t. 7, f. 1-4, t. 8, f. 1-4; Zbid., 1881, clxxi., Pt. 3, p. 
 1037, t. 34, f. 1-2, t. 35, ff. 1-4, t. 36, f. 1-2; Jbéd., 1886, clxxvii., Pt. 1, p. 327, t. 18. 
 Megalania (? Varanus) prisca, Smith Woodward, Ann. and Mag. Nat. Hist., 1888, i., p. 89. 
 Varanus priscus, Lydekker, Cat. Foss. Reptilia and Amphibia Brit. Mus., 1888, Pt. 1, p. 284. 
 ? Megalania (Vertebre, ribs, fibula, and ulna) De Vis, Proc. -R. Soc. Queensland, 1889, vi., Pts. 2 and 3, p. 94. 
 
 Obs. The above name was originally applied by Sir Richard Owen to three 
 vertebre of a land lizard surpassing in bulk the largest existing species, and equal in 
 size to those of the largest living Crocodiles, representing an individual of not less than 
 twenty feet in length. Prof. Owen arrived at these conclusions by a comparison of 
 measurements between the fossils and similar parts of the great Lace Lizard of 
 Australia, Varanus (Hydrosaurus) giganteus, Gray. The vertebre in question were 
 obtained on a branch of the Condamine River, and were purchased for the British 
 Museum. 
 
 The second contribution to our knowledge of this peculiar lizard contained 
 descriptions of an entire dorsal vertebra from the Darling Downs, forwarded to Sir R. 
 Owen by Dr. George Bennett; some-sacral vertebre, and an expanded end of a 
 scapula from the neighbourhood of Melbourne, obtained by Mr. F. M. Raynal; caudal 
 vertebre from Gowrie, Darling Downs, from Mr. St. Jean, with the occipital segment 
 of the skull from the same locality ; and lastly the anterior portion of a skull found by 
 Mr. G. F. Bennett, in 1871, at King’s Creek, Darling Downs. Subsequent to, and 
 including the last discovery, other bones were referred to Megalania by Sir Richard 
 Owen, but unfortunately in his earnest and enthusiastic zeal he united under one name 
 remains from widely separated localities, and obtained at irregular intervals. The 
 oversight which Prof. Owen committed in this respect has been unravelled with 
 marked ability by Mr. Smith Woodward, and I cannot do better than quote his remarks 
 in extenso. Speaking of the cranium found by Mr. G. F. Bennett, he says—“ The latter 
 fragments were hypothetically assigned to the same genus and species + as the original 
 fossils discovered in 1858, and the presence of bony horn-cores upon the skull led to a 
 comparison with the small Australian Jfoloch horridus, which is also provided with 
 dermal horns, though never of an osseous character, A restoration of Megalania was 
 given upon the assumption that the extinct and surviving types were closely allied. In 
 1881 a tail completely ensheathed in bony armour like that of Glyptodon, was found at 
 the same spot in King’s Creek whence had been obtained the fine portion of skull 
 described in the previous year, and this, too, was determined t as belonging to what 
 had now become known as the ‘Great Horned Lizard.’ Uromastix princeps, from 
 Zanzibar, was next compared with the fossil, and Sir Richard Owen pointed out that 
 
 * Restricted, Smith Woodward, 1888. 
 + L.e., Megalania prisea. 
 + Phil. Trans., 1881, clxxii., Pt. 2, p. 547, t. 64. 
 
650 
 
 the caudal armour of this lizard only differed from that of Megalania in the same 
 manner as the horns of Moloch were distinguished from those upon the Queensland 
 skull—namely, in the absence of bony tissue in their structure. The tail of Moloch 
 horridus was also shown to be encased in horny scutes similarly disposed, these even 
 ‘more closely repeating the number and arrangement of Megalania’ than the scutes 
 of Uromastix. Still another contribution was made to the subject in 1886,* when a 
 sacral vertebra from Gowrie, Darling Downs, was described, and also a number of foot 
 bones, supposed to show that Megalania prisca was truly terrestrial, with well developed 
 claws. . . . . A number of fossil remains from a superficial coral-sand formation — 
 in Lord Howe Island . . . . were soon found to comprise parts of an animal 
 very similar to the possessor of the horned bead and armoured tail already known from 
 a locality four hundred miles distant in Queensland. Of these specimens Sir Richard 
 Owen described and figured portions of the skull and mandible, the tail and the partly 
 restored pelvis, besides briefly noticing an anterior vertebra, a portion of a scapula, and 
 a fragment of humerus. He concluded that they belonged to a new sub-genus—perhaps 
 a new genus—to be named Mezolania, comprising apparently two species—M. platyceps 
 and If. minor. Associated with the described fossils, however, were numerous other 
 fragments which Mr. William Davies had placed amongst the Chelonia; and the whole 
 were subsequently re-examined by Professor Huxley, who arrived at the conclusion 
 that they were all Chelonian.t The animal was now considered to be most nearly allied 
 to Chelydra and Gypochelys (Macroclemmys), and other Cryptodiran genera of that 
 type, and Mr. G. F. Bennett’s Queensland skull and tail were unhesitatingly removed 
 from their association with the Megalanian vertebra, and referred to this new genus, 
 for which Professor Huxley thought the name of Ceratochelys would be more appropriate 
 than that of Mecolania. He also re-named Meiolania platyceps, Ceratochelys sthenurus. 
 A new element was thus added to the reptilian fauna of Pleistocene Australia, the 
 Cryptodiran Chelonia being totally unrepresented there, both at the present day and 
 among known fossils from the superficial deposits. Still more satisfactory specimens 
 of Meiolania platyceps afterwards reached Sir Richard Owen, who again presented 
 descriptions to the Royal Society, and concluded that the animal displayed affinities 
 both with the ‘orders Chelonia and Sauria,’ but was more nearly allied to the latter. 
 Another contribution to the correct interpretation of the ‘ Megalanian’ 
 fossils is unwittingly made by Mr. Lydekker in the last volume of his Fossil Mammalia 
 Catalogue just issued. Among the foot-bones assigned to uncertain members of the 
 marsupial families of Notothertide and Phascolomyide are included specimens precisely 
 similar to those described by Sir Richard Owen in Part iv. of his Memoir on Megalania, 
 as affording information in regard to the characters of the feet of this reptile. 
 It thus appears that under ‘ Megalania prisca’ have been included (i.) lacertilian 
 vertebre and an occipital fragment; (ii.) a chelonian skull and tail sheath; and (ii.) 
 marsupial foot-bones. The first necessarily form the type specimens of the genus and 
 species, and the last are obviously at once excluded from consideration. The second 
 series of fossils, however, require a name. 
 
 “Professor Huxley, as already remarked, unhesitatingly places Mr. Bennett's 
 Queensland skull and tail in the same genus as the Lord Howe Island fossils, and the 
 reference appears fully justified by the specimens at present known. . . . . The 
 rules of nomenclature do not permit of the adoption of a new name Ceratochelys, 
 however appropriate it may be, and the genus must henceforth be termed Metolania. 
 
 * Phil. Trans., 1886, clxxvii., p. 327, t. 18-15. 
 + Ibid., p. 471, t. 29 and 30. — 
 } Proc. R. Soc., 1887, xliii., p. 232. 
 
651 
 
 “With regard to species, the figures and descriptions of the Queensland 
 Specimens are at once conclusive of their distinctness from any form yet determined 
 from the distant Lord Howe Island, though they were not specifically distinguished or 
 named by Professor Huxley. They are thus at present nameless; and I would venture 
 to suggest that they may be appropriately known as MJeiolania Oweni.” 
 
 Mr. C. W. De Vis, the able Curator of the Queensland Museum, had, however, 
 without any knowledge of Mr. Smith Woodward's views, arrived at a precisely similar 
 opinion * touching the Lacertilian character of the bones on which Megalania was 
 originally established, and that the “attribution to it of a horned skull is untenable.” 
 
 Notwithstanding the fact that both Messrs. Smith Woodward, Lydekker, and 
 De Vis appear to regard Megalania, Owen, as restricted, simply as a Varanus, or 
 Gigantic Monitor, I have for convenience’ sake, and until the discovery of further and 
 more complete remains, retained the generic appellation. _ 
 
 The vertebre, remarks Mr. R. Lydekker, agree in general character with those 
 of Varanus sivalensis, Falconer, but attain three times the dimensions. 
 
 Loc. and Horizon. Branch of the Condamine Kiver (Colln. Brit. Mus.) ; 
 Gowrie, Darling Downs (Mr. St. Jean)—Fluviatile deposits. 
 
 Genus—V ARAN US, Merran, 1820. 
 (Tent, Syst. Amphib., p. 58.) + 
 
 VARANUS DIRUS, De Vis. 
 Varanus dirus, De Vis, Proc. R. Soc. Queensland, 1889, vi., Pts. 2 and 3, p. 98. 
 
 Obs. Founded on a large Varan tooth, in which the compression usually seen in 
 representatives of this genus is carried to an unusualextent. ‘“‘ Its height and breadth 
 at the base are thrice those of a corresponding tooth of V. varius—wherefore, on the 
 assumption of like proportions throughout, it represents a Varan of about sixteen feet 
 in length.” 
 
 Loc. and Horizon. King’s Creek, Darling Downs (2. W. Frost—Colln. Queensland 
 Mus.)—Fluviatile deposits. 
 
 . VARANUS EMERITUS, De Vis. 
 Varanus emeritus, De Vis, Proc. R. Soc. Queensland, 1889, vi., Pts. 2 and 3, p. 98. 
 
 Obs. Lacertilian remains consisting of portions of a humerus and tibia. The 
 humerus is “from an adult individual, and indicates a species not greatly larger than an 
 average V. varius ; the tibia represents an individual nearly one-half as large again.” 
 
 Loc. and Horizon. King’s Creek, Darling Downs (2. W. Frost—Colln. Queens- 
 land Mus.)—Fluviatile deposits. ° 
 
 Genus—NOTIOSAURUS, Owen, 1884. 
 (Proc. R. Soc., xxxvi., p. 221.) 
 
 NorrosaURUS DENTATUS, Owen. 
 
 Notiosaurus dentatus, Owen, Proc. R. Soc., 1884, xxxvi., p. 221. 
 4s se Owen, Phil. Trans., 1884, clxxv., Pt: 1,.p. 249, t. 12. 
 ? a ne De Vis, Proc. R. Soc. Queensland, 1885, ii., Pt. 1, p. 25, t. 1-3 (humerus and scapula) ; 
 re 33 De Vis, Ibid., 1889, vi., Pt. 2 and 3, p. 97. 
 Obs. The remains of a Pleurodont Lacertilian, consisting of “the outer end of a 
 dentary element of the mandible,” with portions of two teeth zm situ, were described 
 
 
 
 *Proc. R. Soc. Queensland, 1889, vi., Pts. 2 and 3, p. 97. 
 + Fide Lydekker, Cat. Foss. Reptilia and Amphibia Brit. Mus., 1888, Pt, 1, p, 281. 
 
652 
 
 undet the above name from Cuddie Springs, Co. Clyde, New South Wales. These were 
 compared with the living Australian Lizard, Varanus (Hydrosaurus) gigas. Mr. C. W. 
 De Vis has since hypothetically referred to Notiosaurus a left humerus and scapula, 
 representing a reptile with a “ probable length of fifteen feet,” and a tooth. The latter 
 resembles in outline that of Hydrosawrus, but is proportionately thicker. 
 
 The tooth is from Darling Downs, but the localities of the bones are not stated ; 
 but it is quite clear they were obtained at widely separated places, for Mr. De Vis says, 
 speaking of the scapula—‘ which, from wide difference of locality, could not have 
 belonged to the same individual as the humerus.” 
 
 Although the bones described by Mr. De Vis may represent a large Lacertilian, 
 related to Hydrosaurus or Monitor (=Varanus), to place them definitely with the species 
 NV. dentatus is perhaps a little premature. It would have been better to have referred 
 these bones to a distinct genus. 
 
 Loc. and Horizon. The tooth at Clifton, Darling Downs (C. W. De Vis—Colln. 
 Queensland Mus.)—Mr. De Vis informs me that the bones came from Pilton and 
 Chinchilla—Fluviatile deposits. 
 
 Order—CROCODILIA. 
 Family—CROCODILIDZ. 
 
 Genus—OROCODILUS, Laurenti, 1768. 
 (Spec. Med. Exhib. Synop. Reptilium.) 
 
 CrocopiLtus Porosus, Schnerder. 
 Crocodilus porosus, Schneider, Hist. Amphib., Pt. 2, 1801, p. 159. 
 e Lydekker, Cat. Foss. Reptilia and Amphibia Brit. Mus., Pt. 1, 1888, p. 59. 
 
 Obs. The British Museum Collection contains portions of the right maxilla, 
 teeth, dermal scutes, and caudal vertebre, which Mr. R. Lydekker refers to this species. 
 
 Teeth were found by the late Mr. R. Daintree in the Diprotodon-breccias of 
 Northern Queensland, and called by him Crocodilus australis, but in all probability 
 they were those of C. porosus, mentioned in the British Museum Catalogue as presented 
 by “Sir’ R. Daintree.* Mr. Daintree remarked that the Crocodile had, during the 
 Quaternary Period, a greater inland range than it has now. 
 
 Loc. and Horizon. Maryvale Creek, Lat. 19° 80'S. (The late R. Daintree— _ 
 Colln. Brit. Mus.) ; Clifton Plains, Darling Downs (The late Prof. Harkness—Colln. Brit. 
 Mus.); Diprotodon-breccia, Gowrie, Darling Downs (Dr. G@. Bennett—Colln. Brit. 
 Mus.)—Fluviatile deposits. 
 
 Genus—PALLIMNARCHUS, De Vis, 1886. 
 (Proc. R. Soc. Queensland for 1885, ii., Pt. 2, p. 181.) 
 
 PALLIMNARCHUS POLLENS, De Vis. 
 Pallimnarchus pollens, De Vis, Loe. cit.,-p. 191. 
 
 Obs. Speaking of the occasional occurrence of Crocodilian fragments in the 
 Queensland drifts, Mr. De Vis says :—‘‘ Recently, however, more instructive cranial and 
 mandibular fossils have been met with, and it may now be no longer premature to invite 
 
 * Strange to say, the late Mr. Richard Daintree, C.M.G., &c., is frequently spoken of by Mr. 
 Lydekker as “Sir R, Daintree.” The same mistake is committed by Mr. R. A. F. Murray, in his 
 “*Geology and Physical Geography of Victoria.” (S8vo. Melbourne, 1887.) 
 
653 
 
 attention to the evidence they give in favour of two conclusions—first, that the saurian 
 member of the past fauna was not identical with either of the two crocodilians in the 
 present one; second, that it was not even nearly allied to them.’ Portions of the skull, 
 both young and adult, jaws, teeth, and scutes are described. 
 
 Mr. De Vis’ conclusions are—‘‘ No doubt remains that the fossil species was 
 one distinct from the Indo-Australian, and probably ecdemic, Crocodilus porosus on the 
 one hand, and from the saurian peculiar to our northern tableland on the other 
 
 it appears that the portions of skull examined do not, in their imperfect 
 condition, present a combination of characters exclusively alligatorian, nor on the other 
 hand distinctly crocodilian ; but that if we allow this seeming equilibrium of testimony 
 to be disturbed by the weight derived from the imbrication of the scutes, the beam must 
 sink at once on the side of the American family.” 
 
 Loc. and Horizon. Chinchilla, Gowrie Creek, Wiembilla Creek, Condamine River, 
 and Eight-mile Plains, near Brisbane (C. W. De Vis—Colln. Queensland Mus.)— 
 Fluviatile deposits. 
 
 Class—AVES. 
 
 Obs. According to Mr. C. W. De Vis,* twenty-four genera of birds, containing 
 twenty-eight species, are now known from Queensland deposits. Seven of the genera 
 and the whole of the species are considered by him to be extinct. Mr. De Vis 
 remarks :—‘ The extent of the change which the Nototherian avifauna of Queensland 
 is thus shown to have undergone is very much the same as that observed in the case of 
 the marsupials. With two or three very doubtful exceptions, all these have submitted 
 to specific metamorphosis, and of twenty-six of the old genera but fourteen survive. 
 Has the change been rapid? Then, from what cause ? Not from the advent of man; 
 savages do not exterminate. Have we hitherto considered this fauna younger than it 
 really was? Possibly ; but for the solution of these questions we must look to further 
 accumulation and study of paleontological evidence. So far as the Writer can see at 
 present, the Age of the fauna preserved in the Darling Downs Deposits cannot well be 
 later than Early Pliocene.” 
 
 Order—CARINATA. 
 Family—FALCONIDA. 
 
 Genus—TAPHATUS, De Vis, 1891. 
 (Proc, Linn. Soc. N. 8. Wales, vi. (2), p. 123.) 
 
 TAPHETUS BRACHIALIS, De Vis. 
 
 Urotus brachialis, De Vis, Loc. cit., 1889, v. (2), Pt. 4, p. 162. 
 Taphetus brachialis, De Vis, Loc. cit., 1891, vi. (2), Pt. 1, p. 123. 
 
 Ots. The distal half of a humerus and a femur of a diurnal bird of prey are 
 recorded under the above names respectively, given in the synonymy. The humerus 
 was “ the first relic of an arborial bird of flight hitherto recognised amongst the remains 
 of the extinct birds of Queensland.” The femur, on which Mr. De Vis appears to lay 
 the greatest stress, is compared with that of several living genera, and the following 
 description offered:—‘‘ Femur stout (index circ. 9-4), proximal end transversely 
 expanded, shaft compressed, pneumatic foramen small; a rudimentary third trochanter, 
 entepicondylar pit between condyle and epicondyle.” 
 
 Loc. and Horizon. King’s Creek, Darling Downs (0. W. De Vis—Colln. Queens- 
 land Mus.) ; Neighbourhood of Warwick, Darling Downs (H. Hurst—Colln. Queensland 
 
 Mus.) 
 
 
 
 
 
 * Proc, Linn. Soc, N. S. Wales, 1892, vi. (2), Pt. 3, p, 455, 
 
654 
 
 Genus—NECRASTUR, De Vis, 1892. 
 (Proc. Linn. Soc. N. S. Wales, vi. (2), Pt. 3, p. 487.) 
 
 NECRASTUR ALACER, De Vis. 
 Necrastur alacer, De Vis, Loc. cit., p. 437, t. 24, f. la and b. 
 
 Obs. Portion of the proximal end of a right humerus, and the distal end of an 
 ulna representing a bird allied to Nisetus, the Little-crested Eagle. 
 Loe. Darling Downs (C. W. De Vis—Colln. Queensland Mus.) 
 
 Family—PELICANID A. 
 
 Genus—P ELICANUS, Linneus, 1748. 
 (Syst. Nat.) 
 
 PELICANUS PROAVUS, De Vis. 
 Pelicanus proavus, De Vis, Proc. Linn. Soc. N. S. Wales, 1892, vi. (2), p. 444, t. 24, f. 6a and 0. 
 
 Obs. A left tarsometatarsal and a mutilated metacarpal have been identified. by 
 Mr. De Vis as those of a small Pelican. 
 
 Loc. Darling Downs (C. W. De Vis—Colln. Queensland Mus.) 
 
 Family—ARDEID&. 
 
 Genus—PALAOPELARGUS, De Vis, 1892. 
 (Proc. Linn. Soc. N.S. Wales, vi. (2), Pt. 3, p. 441.) 
 
 PALMOPELARGUS NOBILIS, De Vis. 
 Palcopelargus nobilis, De Vis, Proc. Linn. Soc. N. S. Wales, 1892, vi. (2), Pt. 3, p. 441, t. 24, f. 4a and b. 
 
 Obs. The remains of this bird consist of the “distal end of aright ‘medius’ 
 metacarpal in conjunction with that of the ‘ annularis.’ ” 
 
 The metarcarpals most nearly allied to P. nobilis, Mr. De Vis believes to be those 
 of Carphibis and Xenorhynchus, and of these the latter approaches it most nearly in 
 general form and size combined. 
 
 Loe. Darling Downs (C. W. De Vis—Colln. Queensland Mus.) 
 
 Genus—PLATALEA, Linneus, 1766. 
 (Syst. Nat., Ed. xii.) 
 
 PLATALEA SUBTENUIS, De Vis. 
 Platalea subtenwis, De Vis, Proc. Linn. Soc. N. 8. Wales, 1892, vi. (2), Pt. 3, p. 448, t. 24, f. 5a and 6. 
 
 Obs. Proximal two-thirds of a right femur of a supposed Spoonbill. ‘* The 
 specific differences from P. regia and P. flavipes observable in the fossil are a greater 
 flattening of the proximal end of the shaft on its posterior surface, and a diminution 
 of the transverse axis of its distal moiety, resulting in a more cylindrical but more 
 slender form.” 
 
 Lec. Darling Downs (C. W. De Vis—Colln. Queensland Mus.) 
 
655 
 
 Family—ANATID. 
 
 Genus—ANAS, Linneus, 1748. 
 (Syst. Nat.) 
 
 ANAS ELAPSA, De Vis. 
 Anas elapsa, De Vis, Proc. Linn. Soc. N. S. Wales, 1888, iii. (2), Pt. 3, p. 1281, t. 33, f. 4a-c. 
 
 Obs. The presence of Anas amongst the Post-Tertiary fossils of Queensland 
 depends upon the identification of a left tibia and portion of a left femur by Mr. 
 De Vis. The proportions and general appearance of the bones are those of a Teal, and 
 the size about that of Anas punctata. 
 
 Loc. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queens- 
 
 
 
 land Mus.)—Lacustrine or Fluviatile deposits. [‘“ The Chinchilla deposits are beds of 
 sand of considerable but unascertained thickness . . . overlaid by a hard con- 
 glomerate of argillaceous grit and gravel . . . and evidently a lacustrine beach, or 
 
 river bank detritus.”—De Vis. ] 
 
 Genus—DENDROOCY GNA, Swainson, 1837. 
 (Nat. Hist. Birds, p. 365.) 
 
 DENDROCYGNA VALIDIPINNIS, De Vis. 
 Dendrocygna validipinnis, De Vis, Proc. Linn. Soc. N. S. Wales, 1888, iii. (2), Pt. 8, p. 1282, t. 34, f. 5-6. 
 Obs. A Wood-duck is represented by the proximai half of a left humerus, and 
 aright ulna. The bones cannot be identified, says Mr. De Vis, with either of the living 
 
 Australian species. 
 Loc. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queens- 
 land Mus.)—Chinchilla Conglomerate. 
 
 Genus—BIZIURA, Leach, 1824. 
 (Gen. Zoology.) 
 
 Biziura EXHUMATA, De Vis. 
 Bisiura exchumata, De Vis, Proc, R. Soc. Queensland, 1889, vi., Pt. 1, p. 57, t. 4. 
 
 Obs. The fossil to which this name is applied is the left metatarsus of a Duck, 
 agreeing in its massive proportions with the existing genus Biziwra. Itis approximately 
 two-thirds the size of the metatarsus of a male Biziura lobata, Shaw; if, therefore, 
 from an individual of the same sex it would represent a smaller species, but if, on the 
 
 other hand, from a female, a larger one. 
 Loc. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queens- 
 
 land Mus.)—Chinchilla Conglomerate. 
 
 Genus—NYROCA, Fleming, 1822. 
 (Phil. Zool.) 
 
 Nyroca rosusta, De Vis. 
 Nyroca robusta, De Vis, Proc. Linn. Soc. N. S. Wales, 1888, iii. (2), Pt. 3, p. 1278, t. 33, f. 1 and 2. 
 
 Obs. This name was proposed for portions of a right humerus, ulna, and left 
 coracoid, supposed to represent a Nyroca of superior strength to the White-eyed Duck 
 (WV. australis, Gould). “It was a distinctly larger species than its Australian 
 representative in modern days, being one-eighth more in the width of the elbow-joint.” 
 
 Loc. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queens- 
 land Mus.)—Chinchilla Conglomerate. 
 
656 
 
 Nyrroca reciusa, De Vis. 
 
 Nyroca australis et reclusa, De Vis, Proc. Linn. Soc. N. S. Wales, 1888, iii. (2), Pt. 3, pp. 1281 and 1292, 
 ti Osha os 
 
 Obs. A coracoid bone is referred to the recent species WV. australis, Gould. “It 
 is the first instance, within the Writer’s personal experience, of identity, or even of 
 affinity so close, between recent and post-pliocene vertebrates from Darling Downs.” In 
 a postscript, however, reasons are assigned for regarding it as distinct from Myroca 
 australis, and the specific name reclusa is given to it. 
 
 Loc. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queens- 
 land Mus.) —Chinchilla Conglomerate. 
 
 Family—PLOTIDA. 
 
 Genus—PLOTUS, Linneus, 1766. 
 (Syst. Nat., Ed. xii.) 
 
 Protus Pparvus, De Vis. 
 Plotus parvus, De Vis, Proc. Linn. Soc. N. S. Wales, 1888, iii. (2), Pt. 3, p. 1286, t. 35, f. 10a and 6b. 
 
 Obs. A left humerus would appear to indicate the presence of a Darter, with 
 certain affinities to the Pelicanide. ‘‘ Together with the essential traits of Plotus this 
 bone has, as we have seen, a few indications of extraneous aflinity—perhaps we may 
 infer that, as an early form of the genus, it had not attained the high specialisation of 
 its later representative.” 
 
 Loc. and Horizon. Chinchilla, Darling Downs (C0. W. De Vis—Colln. Queens- 
 land Mus.)—Chinchilla Conglomerate. 
 
 Family—COLUMBIDZ. 
 
 Genus—LITHOPHAPS, De Vis, 1891. 
 (Proc, Linn. Soc. N. S. Wales, vi. (2), Pt. 1, p. 121.) 
 
 LIrHoPHAPS ULNARIS, De Vis. 
 Lithophaps ulnaris, De Vis, Loe. cit., p. 122. 
 
 Obs. A genus and species founded on an ulna having the general proportions of 
 the genus Chalcophaps. It is thus described —“ Ulna stout, index 7-88, subcylindrical, 
 continuously arched, with a single row of eight remigial tubercles; arthral surfaces as 
 in Megaloprepia.” 
 
 Loc. and Horizon. Neighbourhood of Warwick, Darling Downs (H. Hurst— 
 
 Colln. Queensland Mus.) 
 Family—GOURIDA. 
 
 Genus—PROGURA, De Vis, 1888. 
 (Proc. R. Soc. Queensland, v., Pt. 4, p. 131.) 
 
 PROGURA GALLINACEA, De Vis. 
 Progura gallinacea, De Vis, Loc. cit., p. 127, 2d. pl., 4 side figs. 
 
 Obs. The presence of a Gouwra or “ Ground Pigeon” during Post-Tertiary times 
 is indicated, according to Mr. De Vis, by four portions of metatarsals. Affinity with 
 the genus Gouwra is “indicated by the shortness of the calcaneal process, sudden 
 attenuation of the inner edge of the bone at its proximal end, elevation of the hind toe, 
 rapid expansion of the distal end, and subsequent descent of the lateral trochleas.” 
 The fossils are twice the size of the corresponding bones of Goura. 
 
 Loc. and Horizon. Chinchilla and Gowrie Creek, Darling Downs* (C. W. De 
 Vis—Colln. Queensland Mus.) . 
 
 * Information supplied by Mr. De Vis. 
 
657 
 
 Family—MEGAPODIDZ. 
 
 Genus—CHOSORNIS, De Vis, 1889. 
 (Proc. R. Soc. Queensland, vi. Pt. 1, p. 55.) 
 
 CHOSORNIS PRETERITUS, De Vis. 
 Chosornis preteritus, De Vis, Proc. R. Soc. Queensland, 1889, vi., Pt. 1, p. 55. 
 
 Obs. Mr. De Vis has proposed this species for the reception of the proximal 
 half of the metacarpus of the left manus of a bird which agrees in several special 
 points with those of the mound-building family. The bone combines features common 
 to both the existing genera Talegallus and Megapodius, with others peculiar to itself. 
 
 Loe. and Horizon. Chinchilla, Darling Downs (0. W. De Vis—Colln. Queensland 
 Mus.)—Chinchilla Conglomerate. 
 
 Family—RALLIDZ. 
 Genus—PORPHYRIO, Brisson, 1760. 
 
 (Ornithologie. )* 
 PorPHyRio ? REPERTA, De Vis. 
 Porphyrio reperta, De Vis, Proc. Linn. Soc. N. S. Wales, 1888, iii. (2), Pt. 3, p. 1288, t. 34, f.7aandb. 
 Obs. A right tarso-metatarsus is referred provisionally by Mr. De Vis to a 
 Coot, near Porphyrio melanotus in size. It may, however, be generally distinct. 
 Loc. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queens- 
 land Mus.)—Chinchilla Conglomerate. 
 
 Porpuyrio Macxintosut, De Vis. 
 
 Porphyrio Mackintoshi, De Vis, Proc. Linn. Soc. N. 8. Wales, 1892, vi. (2), Pt. 3, p. 440, t. 24, f. 2a and 6, 
 
 Obs. The distal extremity of a right tarso-metatarsus indicates a species 
 differing from the preceding in its greater size. Mr. De Vis remarks that probably the 
 present species and Porphyrio reperta will require to be placed in a new genus, in con- 
 sequence of the lesser elevation of the hind toe than in the recent forms of Porphyrio, 
 whilst the inner trochlea in the present fossil is distinctly shorter. 
 
 Loc. and Horizon. Near Warwick (H. Hurst—Colln. Queensland Mus.)— 
 Fluviatile deposits. 
 
 Genus—GALLINULA, Brisson, 1760. 
 (Ornithologie. ) + 
 GALLINULA STRENUIPES, De Vis. 
 
 Gallinula strenuipes, De Vis, Proc. Linn. Soc. N. 8. Wales, 1888, iii. (2), Pt. 3, p. 1284, b. 34, f. 8, 8a, 
 
 Obs. <A left tarso-metatarsus is described by Mr. De Vis under this name. It is 
 a little less than one-fifth longer than the corresponding bone in Gallinula tenebrosa. 
 ‘The evidence given may perhaps be held to show that the bird represented by this bone 
 was a Moor-hen, and one of larger size than the living species.”’ 
 
 Loc. and Horizon. Chinchilla, Darling Downs (0. W. De Vis—Colln. Queens- 
 land Mus.)—Chinchilla Conglomerate. 
 
 GALLINULA PERALATA, De Vis. 
 Gallinula peralata, De Vis, Proc. Linn. Soc. N. 8. Wales, 1892, vi. (2), Pt. 3, p. 440, t. 24, f. 3a and b. 
 Obs. Founded on a humerus possessing an index so far raised as to indicate a 
 bird of superior strength to the recent G. tenebrosa, or the extinct G. strenwipes. 
 Loc. and Horizon. Darling Downs (0. W. De Vis—Colln. Queensland Mus.)— 
 Fluviatile deposits. 
 
 * Fide Agassiz, Nomen. Zool., Fas. 2, p. 31, 
 
 + Agassiz, loc. cit., p. 30. 
 28 
 
658 
 
 Genus—TRIBONYX, Du Bus, 1887. 
 (Bull, Acad. Brux.) 
 
 TRIBONYX EFFLUXUS, De Vis. 
 
 Fulica prior, De Vis, Proc. Linn. Soc. N. 8S. Wales, 1888, iii. (2), Pt. 8, p. 1285, t. 35, f. 90. 
 Tribonyx efluxus, De Vis, Ibid., 1892, vi. (2), Pt. 3, p. 439. 
 
 Obs. The distal end of a humerus was originally figured by Mr. De Vis as that 
 of a Fulica, but it proves to be more properly referable to the above genus. In Fulica, 
 Gallinula, and Porphyrio, the antero-interior side of the trochlea is emarginated, but in 
 Tribonyx it is entire. 
 
 Loc. and Horizon. Chinchilla, Darling Downs (0. W. De Vis—Colln. Queens- 
 land Mus.)— Chinchilla Conglomerate. 
 
 Genus—FULICA, Linneus, 1748. 
 (Syst. Nat.) 
 
 Founica prior, De Vis. 
 Fulica prior, De Vis, Proc. Linn. Soc. N. S. Wales, 1888, iii. (2), Pt. 3, p. 1258, t. 35, f. 9a (non f. 9b). 
 Obs. This name is now restricted, Mr. De Vis informs me, to the proximal end 
 
 of a humerus, formerly associated under the same name with the distal end of another 
 like bone. 
 
 Loc. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queens- 
 land Mus.)—Chinchilla Conglomerate. 
 
 Family—CICONIID 2. 
 Genus—X HNORHYNCHUS, Bonaparte. 
 
 XENORHYNCHUS NANUS, De Vis. 
 Xenorhynchus nanus, De Vis, Proc. Linn. Soc. N. S. Wales, 1888, iii. (2), Pt. 3, p. 1287, t. 35, f. 11 a and b. 
 Obs. The distal half of a right tibia, which resembles that of the Jabiru. 
 Loe. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queens- 
 land Mus.)—Chinchilla Conglomerate. 
 
 Order—RATIT A. 
 Family—DROMO RNITHID A. 
 
 Genus—DROMORNIS, Owen, 1872. | 
 (Proc. Zool. Soc., 1872, p. 682; Trans. Jbéd. 1873, viii., Pt. 4, p. 381.) 
 
 DRroMoRNIS AUSTRALIS, Owen. 
 
 Dromornis Australis, Owen, Proc. Zool. Soc., 1872, p. 682; Tbid., 1887, Pt. 1, p. 95. 
 
 °F; SSCL rans aloud. 1873, Vitisseiate ny p. 381, t. 62, t. 63, f. 1 and 2. 
 Dairies Oweni, Krefft (m.s.), Geol. Mag. , 1874, i., p. 46 (note). 
 Dromornis Australis, Etheridge fil., Cat. Australian Foss., 1878, p. 179 (for synonymy). 
 
 ” “ Owen, Mem. ‘Winaters Birds New Pastane &ce., 1879, p. 467, t. 100, f. 1 and 2. 
 
 99 3 Etheridge fil., Rec. Geol. Survey N. S. Wales, i., Pt. 2, 1889, p. 129, t. 11, f. 1 and 2, 
 t: 12, f. 1 and 25 Jbid., 11,, Pt. 1, 1890, p. 36. 
 
 + mo Lydekker, Cat. Foss. Birds Brit. Mus., 1891, p. 355. 
 
 Obs. The first intimation of the occurrence of a Struthious Bird in the Post- 
 Tertiary deposits of Queensland is due to the late Rev. W. B. Clarke, who announced * 
 the discovery, in 1869, of a femur twelve inches ‘in length, found on 
 sinking a well on the Peak Downs, between Lord’s Table Mountain and the heads 
 of Theresa Creek, and near the track from Clermont to Broadsound. The bone 
 was found in a deposit of drift pebbles and boulders one hundred and fifty feet 
 
 * Geol, Mag., 1869, vi., p. 383, 
 
659 
 
 thick, overlaid by thirty feet of black trappean alluvium. Clarke referred the bone to 
 Dinornis, but in 1872 Sir R. Owen fully described it as a new genus allied to Dromeus, 
 under the name of Dromornis (D. australis, Owen). The remains of Dromornis are 
 also known from New South Wales, for the mutilated femur from the Wellington 
 Caves, figured by Prof. Owen in Mitchell’s “Three Expeditions into the Interior of 
 East Australia,’* is regarded by him as identical with the Queensland bone. It is 
 ’ thirteen inches in length, and was considered by Prof. Owen, from comparative 
 measurements, to represent a bird witha greater stature than the Dinornis elephintopus. 
 
 At the time Mr. Clarke made his announcement the late Mr. G. Krefft referred 
 to the remains of this bird as a Moa, about the size of the Dinornis robustus. He says, 
 “The specimen proving the presence of the gigantic bird, a large femur, was found on 
 the Leichhardt Downs in Queensland, eighty-six feet below the surface, and is now in 
 the Australian Museum.” 
 
 A pelvis of Dromornis was subsequently found in the Canadian Gold Lead, near 
 Gulgong, New South Wales, and a mutilated left tibia at Mount Gambier, South 
 Australia,t both of which were examined, and the latter described by Sir Richard 
 Owen.t His conclusions on the femur and tibia are the following :— 
 
 “The femur, in its essential character, resembles that of the Emu more than it 
 does the similar bone of the Moa,’’ and that “ the characters in which it more resembles 
 Dinornis are concomitant with, and related to, the more general strength and robust- 
 ness of the bone—from which we may infer that the species manifested dinornithic 
 strength and proportions of the hind limbs, combined with the characters of close affinity 
 to the existing smaller, more slender-limbed, and swifter wingless bird peculiar to the 
 Australian continent.’ § 
 
 With regard to the tibia, it need be only stated that there is a nearer resemblance 
 “as in the femur of the gigantic wingless bird of Australia to the genera still there 
 represented (Dromaius and Casuarina) than to Dinornis, Apteryx, or Struthio.”’ || 
 
 In 1889, amongst a collection of bones received at the Geological and Mining 
 Museum, Sydney, from Mr. A. 8S. Cotter, several fragments of bird bones were recognised. 
 The specimens were obtained at a depth of twenty feet from the surface in sinking a 
 well on Caiwarroo Station, near Thargomindah, on the Paroo River. The bird bones 
 consist of portions of the right tibia and left fibula of Dromornis, and part of the right 
 tibia of a Dromaius. 
 
 The Dromornis tibia is the distal extremity of the right bone, obliquely 
 broken as near as possible about the middle of the shaft. The comparative measurements 
 agree fairly well with those of Professor Owen, bearing in mind the relative staté of 
 preservation of the bones. 
 
 ’ 
 Measurements. Owen’s Paroo 
 
 
 
 
 
 
 
 Dromornis, Dromornis, 
 Inches, Lines. Inches. Lines. 
 Transverse breadth of the shaft at the commencement of the | 2 2 2 1} 
 distal expansion | 
 Transverse breadth of the shaft at the commencement of the | 3 5 3 0 
 distal condyles | 
 
 
 
 * 2 Vols. 8vo., London, 1838. 
 
 + Trans. Zool. Soc., 1877, x., Pt. 3, p. 186. 
 
 + For a full history of these discoveries see Clarke, Joc. cit. 
 
 § Trans. Zool. Soc., 1873, viii., Pt. 6, p. 383. 
 
 || Ibid., 1877, x., Pt. 3, No. 8, p. 187. Mr. De Vis informs me that he does not concur in Owen’s view 
 of the affinities of Dromornis, 
 
660 
 
 The bone as preserved is eight and a-quarter inches long, the broken proximal end of 
 the shaft having a diameter of one and eleven-sixteenths inches, with a round oval 
 section. A measurement taken across the precondylar groove, at that point which 
 in Dinornis would be occupied by the bony bridge, gives two and six-sixteenths 
 inches. The anterior surface of the shaft at its proximal end is flattened to some 
 extent, but the posterior is much more convex. The inner lateral surface is also 
 flattened, or may be described as straight-walled, and is margined anteally by an 
 extension of the distal extremity of the procnemial ridge, which is prominent but 
 obtuse. On the anterior surface, the most noticeable feature is the precondylar 
 groove, which is traceable from within two and a-half inches of the broken proximal 
 end of the shaft. The shallow proximal end of this grove is quite contiguous to 
 the inner lateral margin of the shaft, but, as it progresses towards the forepart of 
 the bone, it takes up a median position, as described by Owen. The fossa, or deeper 
 portion between the commencement of the condyles, is more transversely obliquely 
 placed and more open than in the latter’s figure of the left tibia. Its foramen is very 
 much larger than the corresponding pit in the right tibia of Dinornis erassus ; and at 
 the same time there is a most marked difference between the fore and aft thickness of 
 this bone immediately above the position of the bony brilge and that in the first cited. 
 In Dinornis crassus it is one and two-sixteenths inches, but in our Dromornis the 
 measurement reaches one and six-sixteenths inches—i.e., a difference of a quarter of 
 an inch. When the distal pulley-like articular surface is compared with that of 
 Dinornis crassus, very marked differences are perceptible. The inner and upper ends 
 of the condylar ridge on the anterior side approximate closely in Dinornis, but they 
 do not do so in Dinornis crassus, the result being that the intercondylar space or 
 channel is much narrower throughout the whole of its course in Dromornis than in 
 Dinornis crassus. On the outer lateral surface, between the upper edges of the 
 anterior and posterior condylar margins, there is an almost median depression ; 
 this also exists in Dinornis.~ On the contrary, in the Emu and in the Cassowary 
 this is not present, but the surface of the bone is plain and flattened. The 
 bone-substance is thick, measuring at the proximal fracture six-sixteenths of an inch, 
 the central cavity being one inch in diameter, and somewhat less in a contrary 
 direction. ; 
 
 The bone which I refer to the fibula, is in the same state of preservation. It is 
 the proximal end of the left bone, three and a-quarter inches long. The upper articular 
 surface is worn and almost flat and broad; in fact much broader than in the correspond- 
 ing portion of the fibula of Dinornis elephantopus. The outer edge of the head is 
 sharp, and the same side retires inwards, forming a strongly concave surface. The fore 
 and aft measurement of the head is two and fourteen-sixteenths inches, the trans- 
 verse or cross measurement being one and three-quarter inches. The inner side of the 
 fibula in Dinornis elephantopus, between the two inner extremities of the head, is 
 roughly triangularly concave; in the Emu it is elongately concave, but in the present 
 fossil the similar surface is limited, to some extent protuberant, and deeply and closely 
 marked by pits for muscular attachment. 
 
 The posterior prolongation of the head is very marked and long, projecting 
 backwards as an obtuse elongate process, and when compared with the similar part of 
 the fibula of D. elephantopus, is at once seen to be less thick and massive but more 
 projecting. In the Ostrich there is a further diminution, and a still greater in the Emu. 
 The diameter of the shaft of the fibula in the Diénornis elephantopus is one and four- 
 sixteenths inches at a corresponding point to that at which our bone is broken. The 
 same measurement of the latter is only one inch, proving it to be a less powerful bone 
 
661 
 
 at this particular point. The antero-posterior width of the present fossil at the 
 fractured end is one and thirteen-sixteenths inches; that of the bird used above for 
 comparison nearly as possible the same. 
 
 The first point which strikes one is the generally more massive outline of this fibula 
 than that of Dinornis, especially in the wider and larger head. The next peculiarity is 
 the outer and concave smooth surface under the head, which is noticeably different to 
 the structure of the bone both in D. elephantopus and the Emu. 
 
 Loe. and Horizon. Peak Downs between Lord’s Tableland and the head of 
 Theresa Creek (The late Rev. W. B. Clarke—Colln. Australian Mus.); Caiwaroo Station, 
 near Thargomindah, Paroo River (A. S. Cotter—Colln. Mining and Geol. Mus., Sydney) 
 —Fluviatile deposits. 
 
 Family—CASUARIID&. 
 
 Genus—DROMATUS, Vieillot, 1816. 
 
 (Analyse Nouy. Ornith. Elément.) e 
 
 Dromatus Patricius, De Vis. 
 
 Dromaius nove-hollandie, Davies, Geol. Mag., 1884, i. (3), p. 265. 
 a5 patricius, De Vis, Proc. Linn. Soc. N. S. Wales, 1888, iii., Pt. 3, t. 36, figs. 13a-c. 
 Etheridge fil., Rec. Geol. Survey N. S. Wales, i., Pt. 2, 1889, p. 132, t. 11, f. 4, t. 12, 
 f. 3, t. 13, f£. 3; Ibid., ii., Pt. 1, 1890, p. 36. 
 Dromeus patricius, Lydekker, Cat. Foss. Birds Brit. Mus., 1891, p. 352. 
 Dromaius patricius, De Vis, Proc. Linn. Soc. N. 8. Wales, 1892, vi. (2), Pt. 3, p. 446. 
 
 Obs. Under this name Mr. De Vis has described the proximal and distal ends of 
 a right tibia, and a left coracoid, which appear to be distinct from the living Emu 
 (Dromaius nove-hollandie). 
 
 Associated with the remains of Dromornis from the Paroo we have the distal end 
 of aright tibia, which is clearly identical with that of Dromaius patricius, and is probably 
 that of a full-grown bird. Chief amongst the many points of interest is the great 
 development of the extreme distal end of the shaft, where broken, as compared with the 
 condylar portions. That is to say—in the fossil tibia the shaft is much the larger and 
 more solid, but in the recent bone the condyles and portions contiguous are by far the 
 more massive. In the former the cavity of the shaft is fourteen-sixteenths of an inch 
 by eight-sixteenths of an inch, but in the latter these measurements are reduced to 
 twelve-sixteenths and seven-sixteenths respectively. In both the thickness of the bone 
 is the same, two-sixteenths of an inch. The marked difference in the size of the two 
 bones appears to have also struck Mr. De Vis, and is expressed in his description of the 
 distal end of the tibia. 
 
 Mr. R. Lydekker ascribes my specimen to New South Wales, but the locality 
 whence it is derived is in Queensland. 
 
 Loc. and Horizon. King’s Creek, Darling Downs (C. W. De Vis—Colln. 
 Queensland Mus.) ; Caiwaroo Station, near Thargomindah, Paroo River (A. S. Cotter— 
 Colln. Mining and Geol. Mus., Sydney) —Fluviatile deposits. 
 
 +B) ” 
 
 DROMAIUS GRACILIPES, De Vis. 
 Dromaius gracilipes, De Vis, Proc. Linn. Soc. N. 8. Wales, 1892, vi. (2), p. 445, t. 23, £. 7a-b. 
 
 Obs. The distal extremity of a metatarsus smaller and slimmer than that of the 
 living D. nove-holiandie, has prompted the establishment of the present species ; nor 
 does any trace of the plantar artery canal, or of the tunnel or groove for the 
 descending branch of the artery exist. The above species, D. patricius, is intermediate 
 
 
 
 * Fide Agassiz, Nomen. Zool., Fas. 2, p. 26. 
 
662 
 
 in the latter characters, the plantar perforation being exceedingly small; not greater 
 than the diameter of an ordinary pin. In all probability D. gracilipes was not only 
 rmaller than the Emu, but also more attenuated in the proportions of its limb. 
 
 Loc. and Horizon. Darling Downs (0. W. De Vis—Colln. Queensland Mus.)— 
 Fluviatile deposits. 
 
 Family—DINORNITHID&. 
 
 Genus—DINORNIS, Owen, 1844. 
 (Trans. Zool. Soc., iii., Pt. 3, 235.) 
 
 DINORNIS QUEENSLANDI&, De Vis. 
 Dinornis queenslandice, De Vis, Proc. R. Soc. Queensland, 1884, i., Pt. 1, p. 28, t. 3 and 4. 
 =f 7 Lydekker Cat. Foss. Birds Brit. Mus., 1891, p. 222. 
 p > De Vis, New Zealand Journ. Sci., 1891, i. (2), No. 3, p. 97. 
 
 Obs. The presence of a species of Moa during Post-Tertiary times in Queensland 
 has been inferred by Mr. C. W. De Vis from the characters of a struthious femur in the 
 Queensland Museum. The specimen presents precisely the measurements of Déinornis 
 erassus, Owen, aud Mr. De Vis adds —“ The large air channel into the interior bone of 
 the Emu, so intimately connected with the excursive habits of the typical birds, is wanting 
 in all the fossils under consideration, but in the Moa, and in our fossil alike, it is fore- 
 shadowed by three small foramina just beneath the hinder edge of theneck. .... The 
 chief particulars in which the femur differs from that of Dromornis, are a long sloping 
 neck, constricted at its junction with the head, a full and irregularly oval shaft, and a 
 broad outer trochanterian surface. These are precisely the characters by which the 
 corresponding part of the thigh-bone of Dinornis is differentiated by Sir R. Owen from 
 that of Dromornis, and in all of them our fossil agrees almost exactly with the femurs 
 of D. crassus and D. elephantopus.” 
 
 I am indebted to the courtesy of Mr. De Vis for a reproduction of this fragmentary 
 bone. A very careful comparison with the femur of a Dinornis and with the type of 
 Dromornis compels ine to admit the close resemblance between his bone and the former. 
 On it Mr. R. Lydekker also remarks—-“This specimen appears indistinguishable 
 from the femora of true Dinornithide, and is quite different from the femur of 
 Dromornis.”’ 
 
 Loc. and Horizon. King’s Creek, Darling Downs (J. Daniels—Colln. Queensland 
 Mus.)—F luviatile deposits. 
 
 Family—APTERYGIDA. 
 
 Genus—METAPTERYX, De Vis, 1892. 
 (Proc, Linn. Soc. N. 8. Wales, vi. (2), Pt. 3, p. 453.) 
 
 METAPTERYX BIFRONS, De Vis. 
 Metapieryx bifrons, De Vis, Loc. cit., p. 453, t. 23, f. 8a and b. 
 
 Obs. The distal half of a tarso-metatarsus, on careful comparison with the similar 
 bone in the Apteryx, seems to “ justify the conclusion that in spite of all our preconcep- 
 tions this Australian relic represents a bird having a decided family relationship with 
 the Apterygide of New Zealand.” The more striking features in which it appears to 
 resemble the Apteryx are the great distal extension of the pedicels of the trochlee, a 
 like equality in the length of the opposed surfaces of the lateral pedicels, and the exten- 
 sion of the mesial trochlea beyond the extremities of the other two, &c. It is, however, 
 not an Apteryx, as is evinced by the absence or rudimentary state of the hind toe, the 
 
663 
 
 superior length of the inner one of the lateral toes, and the enlargement of the middle 
 one out of all proportion to the laterals. Although WZ. bifrons did not exceed the living 
 Kiwis in stature, its cursorial power was much greater, and it may be inferred that the 
 bird was as much an Emu as an Apterye. 
 
 Loc. and Horizon. Darling Downs (0. W. De Vis—Colln. Queensland Mus.)— 
 Fluviatile deposits. 
 
 Class—M AMMALIA. 
 
 Order—MONOTREMATA. 
 Family—ECHIDNID. 
 
 Genus—ECHIDNA, Cuvier, 1797. 
 (Tabl. Eléméntaire, p. 143.) 
 
 Ecuipna Owentt, Krefft. . 
 
 Echidna Owenii, Krefft, Ann. and Mag. Nat. Hist., 1868, i., p. 113, f. 1-5. 
 3 re Krefft, Australian Vert. Fossil and Recent, 1871, p. 22. 
 . Ramsayt, Owen, Phil. Trans., 1884, clxxx., Pt. 1, p. 273, t. 14. 
 $5 Owenii, Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 295. 
 
 Oés. The late Mr. G. Krefft figured a fragment of a humerus of larger size than 
 the corresponding bone of the existing Echidna, to which he applied the above name. 
 
 Sir Richard Owen has since described the remains of an Echidna from the 
 Wellington Valley Caves as #. Ramsay, but he made no comparison between his own 
 and Mr. Krefft’s fossils. It is, however, probable that Mr. Richard Lydekker is correct 
 in uniting both in one species. He remarks—‘ Considerably exceeding in size the exist- 
 ing E. Bruijniit of New Guinea.” Sir Richard Owen’s type was obtained in the 
 ossiferous breccia of the Wellington Caves. 
 
 Loc. and Horizon. Darling Downs (The late G. Krefft—Colln. Australian 
 Museum)—Fluviatile deposits. 
 
 Family—ORNITHORHYNCHID. 
 
 Genus—ORNITHORH YNCHUS, Blumenbach, 1800. 
 (Voigt’s Magazin.)* 
 
 ORNITHORHYNCHUS AG@ILis, De Vis. 
 Ornithorhynchus agilis, De Vis, Proc. R. Soc. Queensland, 1885, ii., Pt. 1, p. 35, t. 4, f. 1-3. 
 
 Obs. The existence of the Platypus in Post-Tertiary times in Queensland is 
 believed by Mr. De Vis to be assured from the presence of an adult right tibia. “It 
 shows no sign of having been inherited from a less modified, that is, more reptilian 
 precursor ; on the contrary, it possesses all the character of the genus as represented by 
 [0.] paradoxus, fully matured, and even more pronounced than in its descendant. It is, 
 perhaps, worthy of remark that, presuming this tibia to be full-sized as well as adult, it 
 indicates a species of smaller dimensions than the present one.” The bone is even thought 
 to represent a distinct and undescribed genus. 
 
 A mandible was also collected at the same locality which corresponds in repre- 
 senting a smaller species than the living O. anatinus. 
 
 Messrs. Flower and Lydekker appear to have entirely overlooked the occurrence 
 of this extinct species in their otherwise excellent account of the “ Duck-billed Platypus.” + 
 
 Loc. and Horizon. Near Pilton, King’s Creek, Darling Downs (0. W. De Vis— 
 Colln. Queensland Museum) — Fluviatile deposits. 
 
 * Fide Agassiz, Nomenclator Zool., Fas. 1, p. 23. 
 + Introd. Study of Mammals, Living and Extinct, 1891, p. 119. 
 
664 
 
 Order—MARSUPIALIA. 
 Family—PHASCOLOMYID&. 
 
 Genus—PH ASCOLOM YS, Geoffroy, 1803. 
 (Ann. Mus. Hist. Nat. Paris, ii., p. 365.) 
 
 Obs. The extinct Wombats may be divided, as they have been to a certain 
 extent by Sir R. Owen, into two groups—those of equal or less size than the existing 
 Species, and those exceeding the latter. In the first division we have P. medius, Pe 
 magnus, and P. gigas; in the second one, P. Mitchelli, P. parvus, P. platyrhinus, 
 and P. Thomsoni. Professor Owen states that we are now acquainted with species of 
 Phascolomys exhibiting “gradations of bulk rising from that of a Marmot to that of a 
 Tapir ;” butit is quite open to doubt if the gigantic species burrowed, like their more 
 recent and smaller brethren. 
 
 PHASCOLOMYS MEDIUS, Owen. 
 
 Phascolomys medius, Owen, Phil. Trans., 1873, clxii., Pt. 2, p. 241, t. 32, f. 2-7, t. 33, f. 2-6, t. 34, t. 35, £. 7. 
 Owen, Extinct Mam. Australia, 1877, pp. 339 and 353, Atlas, t. 57, f. 2-7, t. 58, f. 2-6, 
 f. 59, t. 60, f. 7. 
 np of Lydekker, Cat. Foss, Mam. Brit. Mus., 1887, Pt. 5, p. 149. 
 
 Obs. Lower and upper jaws of this species have been discovered, indicating a 
 Wombat larger than either of the two largest existing species. The lower jaw must 
 have been six or seven inches in length, and the entire animal when full grown one-half 
 larger than P. platyrhinus. 
 
 Loe. and Horizon. Condamine River at Eton Vale, Darling Downs (Z. 8. Hill 
 —Colln. Brit. Mus.) ; King’s Creek, Darling Downs (Mr. Turner—Colln. Brit. Mus.) ; 
 Drayton, Darling Downs (Sir D. Oooper—Colln. Brit. Mus.)—Fluviatile deposits. 
 
 Ya 
 
 9 ” 
 
 PHASCOLOMYS MAGNUS, Owen. 
 
 Phascolomys magnus, Owen, Phil. Trans., 1878, clxii., Pt. 2, p. 246, t. 35, f. 1-6. 
 Owen, Extinct Mam. Australia, 1877, pp. 344-346, and 353, t. 60, f. 1-6. 
 5 Fe) Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 148. 
 Obs. The disposition of the upper molars in this species resembles that of 
 P. medius, and is of the type of the existing Hairy-nosed Wombat. 
 Loc. and Horizon. Eton Vale, Darling Downs (£. S. Hzll—Colln. Brit. Mus.) ; 
 Drayton, Darling Downs (Sir D. Cooper—Colln. Brit. Mus.)—Fluviatile deposits. 
 
 Phd ” 
 
 PuHascotomys MircHeit, Owen. 
 
 Phascolomys Mitchelli, Owen, Mitchell’s Three Expeds. Int. E. Australia, 1838, ii., p. 362, t. 30, f. 4-6. 
 
 Owen, Phil. Trans., 1873, clxii., Pt. 2, pp. 177, 179, 181, 182, and 191, t. 17, f. 1, 3-5, 
 7 and 8, t. 18, f. 1-7,.t. 19, £. 5, t. 21, £. 5 and 6. 
 
 Owen, Extinct Mam. Australia, 1877, pp. 318, 320, 322, 324, 332, and 358, t. 50, f. 1, 
 3; 5, 7, and 8, t. 51, £. 1-7, t. 53, £. 5, t. 55, f. Dand:6; 
 
 Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 152. 
 
 on A De Vis, Proc. Linn. Soc. N. S. Wales, 1891, vi. (2), Pt. 2, p. 239. 
 
 Obs. This species agrees more or less in size with the existing Wombats, and is 
 close to P. platyrhinus. Mr. C. W. De Vis has quite recently afforded strong evidence of 
 the satisfactory specific importance of this species, by describing numerous bones other 
 
 than those of the cranium. 
 Loc. and Horizon. Gowrie, Darling Downs (Ff. NV. Isaac)—Fluviatile deposits. 
 
 ” ” 
 
 ” ” 
 
 3” ” 
 
665 
 
 PHASCOLOMYS PARVUS, Owen. 
 Phascolomys parvus, Owen, Phil. Trans., 1873, clxii., Pt. 2, p. 193, t. 19, f. 6 and 7; t. 20, f. 6-8, t. 23, f. 6 
 and 7, t. 38, f. 5 and 6. 
 
 ” + Owen, Extinct Mam. Australia, 1877, pp. 334 and 353, Atlas, t. 53, f. 6 and 7, t. 54, 
 f. 6-8, t. 56, f. 6 and 7, t. 63, f. 5 and 6. 
 ” of Lydekker, Cat. Foss. Mam, Brit. Mus., 1887, Pt. 5, p. 156. 
 
 Obs. Although a small species, does not agree with the smallest known living 
 form, the Tasmanian Wombat. 
 
 Loc. and Horizon. King’s Creek, Darling Downs (Mr. Turner—Colln. Brit. 
 Mus.)—Fluviatile deposits. 
 
 PHASCOLOMYS PLATYRHINUS, Owen. 
 Phascolomys platyrhinus, Owen, Phil. Trans., 1873, clxii., Pt. 2, pp. 175, 180, 198, t. 19, f. 2, t. 20, f. 3-5, 
 
 t. 21, f. 2, t. 23, f. 1 and 8—cuts p. 175, f. 1, p. 179, f. 5, and p. 180, f. 7. 
 
 » 53 Owen, Extinct Mam. Australia, 1877, pp. 328-334, and 353—cuts p. 316, f. 3, 
 Dercc ie Os) Paoelet te (anty Dest. oa Galo; te 0 oe lotta oo, ty DD, ft. 2, 
 t. 56, f. Land 8, t.58, f. 1, t: 98, £.3, 4, and 13, t. 99; £3 and 4, t. 100, 
 f. 4-6 and 8, t. 101, f. 3, 4, and 10, t. 102, f. 2, 4, and 6. 
 
 ” Hf Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 155, 
 
 Obs. The shape and proportions of the molars seen in the living examples of 
 this species, says Prof. Owen, are closely preserved in the fossil forms. The researches 
 of Mr. C. W. De Vis * amongst the Darling owns Phascolomydw# have rendered it 
 exceedingly doubtful if this species is represented in ithe ossiferous deposits of that 
 district, the remains hitherto ascribed to P. platyrhinus being in all probability those 
 of P. Mitchelli. 
 
 Loc. and Horizon. Eton Vale, Darling Downs (#. S. Hili—Colln. Brit. Mus.) 
 —Fluviatile deposits. 
 
 PHascotomrys THomsoni, Owen. 
 Phascolomys Thomsont, Owen, Phil. Trans,, 1873, clxii., Pt. 2, p. 192, t. 18, f. 8 and 9, t, 21, f. 7. 
 ” ? Owen, Extinct Mam. Australia, 1877, pp. 333 and 353, t. 51, f. 8 and 9, t. 55, f£. 7. 
 Fr, A; Lydekker, Cat, Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 156. 
 
 Obs. The critical examination of the Darling Downs fossil Wombat remains, 
 already referred to, has led Mr. De Vis to the conclusion that this supposed species has 
 no existence. He remarks t—‘ P. Thomsoni, Ow., is an extremely doubtful species, 
 uniquely represented, and dependent for its validity upon a single character, the. 
 backward extension of the symphasis, a character which varies with age. 
 
 P. Thomsoni should, therefore, be expunged from our lists.” 
 
 Loc. and Horizon. Drayton, Darling Downs (Sir D. Cooper—Colln. Brit. 
 
 Mus.)—Fluviatile deposits. 
 
 PHASCOLOMYS ANGUSTIDENS, De Vis. 
 Phascolomys angustidens, De Vis, Proc. Liun. Soc. N. S. Wales, 1891, vi. (2), Pt. 2, p. 243. 
 
 Obs. Established by Mr. De Vis for a Wombat distinguished by the narrowness 
 of its teeth, “which are intermediate in breadth between those of P. parvus and 
 P. Mitchelli, though serially as long or longer than in the latter species. As a marked 
 reduction in the width of the teeth has not been noted in the descriptions of known 
 species, and as the teeth in all the mandibles of P. Mitchelli are appreciably the same 
 in width, I must perforce regard this narrow-toothed wombat as a new species.” A 
 . humerus anda tibiaare also referred to P. angustidens. The animal is supposed to have 
 been equal in size to P. Mitchelli, but more delicate in structure. 
 
 Loc. and Horizon. Valley of the Condamine, Darling Downs (C. W. De Vis— 
 Colln. Queensland Mus.)—F luviatile deposits. 
 
 * Proc. Linn. Soc. N. 8. Wales, 1891, vi. (2), Pt. 2, p. 239. 
 + Loc. cit., p. 239. 
 
666 
 
 Genus—P HASCOLONUS, Owen, 1872. 
 (Phil. Trans., clxii., p. 248.) 
 
 PHASCOLONUS GIGAS, Owen. 
 
 Phascolomys gigas, Owen, Encyclop. Brit., 1859, xvii., p. 175, f. 114. 
 os (Phascolonus) gigas, Owen, Phil. Trans., 1873, clxii., Pt. 2, pp. 248 and 255, t. 36-38, f. 1, 3, and 
 4, t. 39, f. 1-3, t. 40. 
 
 ” ” 5» Owen, Extinct Mam. Australia, 1877, p. 346, t. 61-63, f. 1, 3, and 4, t. 64, 
 f Sri GD. 
 Phascolonus gigas (pars.), Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 157. 
 55 »» De Vis, Proc. Linn. Soc. N. S. Wales, 1891, vi. (2), Pt. 2, p. 237. 
 
 Obs. For this gigantic Wombat, equalling as it did the Wild Ass in size, Prof. 
 Owen has proposed the sub-generic name of Phascolonus, but both Mr. Lydekker and 
 Mr. C. W. De Vis have raised it to generic rank. 
 
 Loc.and Horizon. King’s Creek, Darling Downs (The late OC. H. Hartmann—Colln. 
 Brit. Mus.) ; Gowrie, Darling Downs (Sir D. Cooper—Colln. Brit. Mus.) ; Eton Vale, 
 Darling Downs (Z. 8. Hill—Colln. Brit. Mus.) ; Tributary of the Condamine River, St. 
 Jean Station (S. St. Jean—Colln. Australian Mus.) ; Clifton Plains, Darling Downs 
 (Str F. Nicholson—Colln. Queen’s College, Cork)—Fluviatile deposits. 
 
 Family—NOTOTHERIIDZ, 
 
 Genus—NOTOTHERIUM, Owen, 1845. 
 (Brit. Assoc. Report for 1844, p. 231.) 
 
 Obs Nototherium is second only in bulk to Diprotodon. The skull of the 
 former is shortcr in proportion to its breadth and depth than that of the latter. 
 Nototherium resembles the Koala and Wombats, whilst Diprotodon is more nearly 
 allied in many of its characters to the Kangaroos.* Nototherium does not possess 
 incisors of the relative sizé and shape and persistent growth characteristic of Dipro- 
 todon, but it surpasses the latter in both absolute and relative size of the zygomatic 
 arches. 
 
 The dental formula of Wototheriwm is 7. +, ¢. 0-0, m. 8:3, = 28. 
 
 By some Authors Zygomaturus, Macleay, is considered as distinct from Woto- 
 therium, but Sir R. Owen believes them to be identical. Recently Mr. De Vis has 
 revived this question, and arrives at the following conclusions :—lst. That the upper 
 premolar of Nototherium shows a departure not more than generic from that of 
 Diprotodon, and consequently that both genera belong to one family, the Nototheriida, 
 which also includes Luowenia, and perhaps Sthenomerus. 2nd. That Zygomaturus is a 
 good genus, and its affinity with the Nototheriide is, to say the least, doubtful. 
 3rd. The mandibular structure and dentition of Zygomaturus are, as yet, unknown, as 
 it was one of the rarer animals of its day, the paucity of its remains contrasting 
 strongly with the abundance of those of Nototherium. These conclusions have been 
 combated by Mr. R. Lydekker,t who regards the previous determination of Owen, 
 that Mototherium and Zygomaturus are one and the same, as correct. 
 
 Mr. De Vis has also described a humerus which he axscribes to Notothertum.§ 
 
 * Mr. De Vis informs me that he considers that this view is by no means favoured by the pelvis and 
 foot-bones, which are essentially phascolomine. Notwithstanding its molar system Dzprotodon is far more 
 a.Wombat than a Kangaroo. 
 
 + Note on the Genera Zygomaturus and Nototheriwm. Proc. R. Soc. Queensland, 1888, v., Pt. 3, p. 111. 
 
 { Ann. and Mag. Nat. Hist., 1889, iii., p. 149. 
 
 § Proc. Linn. Soc, N, S. Wales, 1883, viii., Pt, 3, p. 404. 
 
667 
 
 NotrorHertum MitcHEni, Owen. 
 Nototherium Mitchelli, Owen, Brit. Assoc. Report for 1844 [1845], p. 232. 
 
 » i Owen, Phil. Trans., 1872, clxii., Pt. 1, pp. 41, 52, 60, 66, and 82, t. 2, f. 1 and 2, t. 3, 
 frleo, tad, Dy and G, te Om tel-4G-5. t10, £& 1-3) 7 and &, t, 11> p, 42; & 1; 
 p. Gl, £ 2. ; 
 
 ” S Qwen, Extinct Mam. Australia, 1877, pp. 249, 272, 514, t. 36, f. 1 and 2, t. 37, 
 
 f. 1-3, tt. 38, 39, 40, t. 43, f. 1-4, 6-8, t 44, f. 1-3, 7 and 8, t. 45, t. 88 f. 
 11-14, p. 250, f. 1, p. 269, f. 2. 
 
 ” = Owen, Quart. Journ. Geol. Soc., 1882, xxxviii., p. 394, t. 16. 
 
 ” a (pars.), Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 163. 
 
 Obs. The skull, without a lower jaw attached, from King’s Creck, presented to 
 the Australian Museum by Mr. F. N. Isaac, and upon which Mr. Macleay established 
 his genus Zygomaturus, Prof. Owen says, belongs to the same species as the lower jaw 
 originally described by him from the same locality as Nototherium Mitchelli. The 
 latter is now in the British Museum, and was purchased after being sent to London by 
 Mr. Boyd. 
 
 Loc. and Horizon. King’s Creek, Darling Downs (Restored Skull—Colln. 
 Brit. and Australian Mus.) ; Eton Vale, Darling Downs (Z. S. Hili—Colln. Brit. 
 Mus.) ; Gowrie Creek, Darling Downs (H. Hughes—Colln. Worcester Nat. Hist. Soc.); 
 Albert River (R. Daintree—Colln. Brit. Mus.) ; Warra Warra Station, Condamine 
 River (Dr. G. Bennett—Colln. Brit. Mus.)—Fluviatile deposits. 
 
 NorToTHERIUM INERME, Owen. 
 Nototherium inerme, Owen, Brit. Assoc. Report for 1844 [1845], p. 231. 
 
 3 An Owen, Phil. Trans., 1872, clxii., Pt. 1, pp. 41, 43, and 67, t. 8, t. 9, f. 5. 
 += rh Owen, Extinct Mam. Australia, 1877, pp. 271 and 514, t. 42, t. 43, f. 5, t. 88, f. 15-17, 
 Ue bey 
 
 Obs. The specific difference of WV. inerme from the other two species of the genus 
 is shown in the relative position of the symphysis to the fully-developed molar series. 
 The name refers to the absence of incisor tusks. 
 
 Mr. Lydekker includes both this species and WV. victorie, Owen, as synonyms of 
 N. Mitchelli.* 
 
 Loc. and Horizon. Gowrie, Darling Downs (G. F. Bennett—Colln. Brit. Mus.) 
 —Fluviatile deposits. 
 
 NotrotHERIUM DUNENSE, De Vis. 
 
 Nototherium dunense, De Vis., Proc. Linn. Soc. N. 8. Wales, 1587, ii. (2), Pt. 4, p. 1065, t. 38. 
 . 9 De Vis, Proc. R. Soc. Queensland, 1888, v., Pt. 3, p. 116, 2nd Pl., centre figs. 
 
 Obs. A mandibular fragment and a left adult mandibie have been separated by 
 Mr. De Vis as representing another species of Mototherium. It is distinguished from 
 N. Mitchelli, Owen, “by the size and structure of the premolar and position of the 
 inlet of the dental canal”; from WV. inermis, Owen, “ by the development of the tusks 
 and consequent retrocession of the symphysial curve”’; and from D. Victorie, Owen, 
 “by the position of the inlet of the dental canal and by the gradual enlargement of the 
 molars serially.” 
 
 Loc. and Horizon. Darling Downs (C. W. De Vis — Colln. Queensland Mus.)— 
 
 Fluviatile deposits. ° 
 
 
 
 * Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 162. 
 
668 
 
 Genus—DIPROTODON, Owen, 1838. 
 (Mitchell’s Three Exped. Int. E. Australia, ii., p. 362.) 
 
 DIPROTODON AUSTRALIS, Owen. 
 
 Diprotodon australis, Owen, Loe. cit., p. 362, t. 31, f. 1 and 2. 
 Mastodontoid Pachyderm, Owen, Ann. and Mag. Nat. Hist., 1843, xi., pp. 8 and 9, f. 2 and 3 (non f. 1). 
 Dinotheriwm australe, Owen, Ibid., p. 329, f. 1, p. 330, f. 2. 
 Diprotodon australis, Owen, Brit. oon Report for 1844 {1845}, p. 224. 
 . ¥ Owen, Phil. Trans., 1870, clx., Pt. 2, p. 519, t. 35, f. 1-4, t. 36-39, t. 40, f. 1-13, 16-18, 
 t. 41-50. 
 x an Owen, Extinct Mam. Australia, 1877, pp. 189 and 507, t. 19, f. 1-4, t. 20, 23, and 24, 
 f. 1-13, 16-18, t. 25-35, t. 122, f. 1-3, 7-10, t. 123 and 124, and frontispiece—cuts, ni 
 land la, p. 189, f. 2, p. 204, “ D; p: 212, £26; p. 219. 
 a 33 Etheridge fil., Cat. Australian Foss., 1878, p. 180 (for full synonymy). 
 
 Obs. Diprotodon combines the characters of the genera Macropus and 
 Phascolomys, but with special modifications of its own, more particularly exhibited in 
 the bones of the trunk and limbs. The pelvis and femora present resemblances to the 
 Proboscidex not hitherto observed in any other remains of large extinct quadrupeds in 
 Australia. In all the bones, setae essentially marsupial characters are visible. 
 
 The dental formula is z. 8-8, ¢. 0:0, m.$3,=28.* 
 
 Sir Richard Owen has a one -one occasions on which the remains of 
 this large marsupial have been found throughout Australia ¢; of these discoveries no 
 
 less than thirteen refer to Queensland, viz. :— 
 
 1. Tributaries of the Condamine River in a deep bed of alluvium; Sir T. L. 
 Mitchell, 1842. 
 2. Hodgson, Campbell, Isaac, and Oaky ein Condamine River, either in 
 red loamy breccia, or a bed of pebbles; L. Leichhardt, 1844. 
 3. King’s Creek, Darling Downs ; — Turner, 1847. 
 4, Isaac’s Creek, Gowrie, Darling Downs; F. WV. Isaacs, 1849. 
 5. Galtindaddaiy Melville Plains; W. Buchanan, 1851. 
 6. Creeks, Darling Downs; H. Hughes, 1856. 
 7. Gowrie, Darling Downs; J. #. Allport, 1869. 
 8. Condamine Valley, 100 feet below surface; J. H. Hood, 1861. 
 9. Eton Vale, Darling Downs; £#. S. Gill, 1863. 
 10. St. Ruth’s Station, Condamine River; H. Campbell, 1865. 
 11. St. Jean Station, Condamine River; S. St. Jean, 1865. 
 12. Clifton Plains, Darling Downs; F. Nicholson, 1866. 
 13. King’s Creek, Clifton Station, Darling Downs; G. F. Bennett, 1877 (about). 
 
 This list of localities does not appear to include that of the original skull sent to 
 London by Mr. Boyd and purchased for the British Museum. It was from the ‘ bed of 
 a creek at Gowrie, near Drayton, Darling Downs,” and is probably identical, says Sir 
 R. Owen, with the head referred to by Dr. G. Bennett as found by a shepherd on King’s 
 Creek. 
 
 To the above must be added the discovery of Diprotodon remains in brecciated 
 alluvium by the late Mr. R. Daintree, on Maryvale Creek, Clarke River. 
 
 Loc. and Horizon. As given above—Fluviatile deposits. 
 
 
 
 * Proc. R. Soc., 1870, xvii., p. 196. 
 
 + Phil. Trans., 1870, clx., p. 570; Extinct Mam. Australia, 1877, pp. 240 and 507. The numerous 
 localities at which Diprotodon remains have been found by the Geological Survey of New South Wales and 
 Collectors in South Australia and Queensland are not included here. 
 
 ~ Quart. Journ. Geol. Soc., 1872, xxviii., Pt. 3, p. 274. 
 
669 
 
 Diprotopon minor, Huzley. 
 
 Diprotodon minor, Huxley, Quart. Journ. Geol. Soc., 1862, xviii., p. 422, t. 21, ff. 4-6:* 
 Nototherium, sp., Owen, Extinct Mam. Australia, 1877, p. 511. 
 Diprotodon minor, Etheridge fil., Cat. Australian Foss., 1878, p. 181. 
 
 » % De Vis, Proc. R. Soc. Queensland, 1888, v., Pt. 2, p. 38, Pl., top figs. 
 
 Obs. The fossils described by Prof. Huxley as representing a small species of 
 Diprotodon appear to be regarded by Sir R. Owen as a Notutherium, it we may judge 
 by the very brief remarks he makes in his “‘ Extinct Mammals of Australia.” Latterly 
 Mr. De Vis has studied Diprotodon minor, and states that both of the species figured by 
 Huxley “ were in 1887 identified by Sir R. Owen with ascertained species of his genus 
 Nototherium ; D. (australis?) was figured as N. Mitchelli, D. minor as N. victoria.” 
 
 I have failed to find any identification of this kind by Prof. Owen, who 
 simply suggests to the reader a comparison of Huxley’s D. minor with his Nototherium 
 Mitchelli. The conclusions arrived at by Mr. De Vis are as follows :—“ The premolars 
 figured by Professor Huxley are unmistakably those of Diprotodon. The distinctness 
 of the animal they represent from D. australis, affirmed with some reserve by Prof. 
 Huxley, and practically without reserve by Sir R. Owen, is confirmed by fresh evidence. 
 The differences between the three premolars made known are reconcilable, the difficulty 
 raised by them less than that of admitting three allied species in the same habitat. 
 They represent one form, 7). minor, which is a species, and not the female of D. australis. 
 The genus therefore combines two species, D. australis, Ow., and D. minor, Hux.” 
 
 Loc. and Horizon. Gowrie, Darling Downs (Ff. NV. Isaac)—F luviatile deposits. 
 
 Genus—HUOWENTA, De Vis, 1891. 
 
 Owenia, De Vis, Proc. R. Soc. Queensland, 1887, iv., p. 100 (non Presch, nec Kolli cker). 
 Euowenia, De Vis, Proc, Linn. Soc. N. S. Wales, 1891, vi. (2), Pt. 2, p. 160. 
 
 Evowenta Grata, De Vis. 
 
 Owenia grata, vik Proc. R. Soc. Queensland, 1887, p. 100, t. 1-4; Jbid., 1888, v., Pt. 3, 2nd plate (lower 
 8). 
 
 Euowenia grata, De ey Proc. Linn. Soc. N. S. Wales, 1891, vi. (2), Pt. 2, p. 160 and 165. 
 
 Obs. A new genus of Diprotodontide, with the dental formula 7. 2, p.m. 4, 
 m. +. <A full description will be found in the Author’s Paper “ On an Extinct Mammal 
 of a Genus apparently new.” From this the following general remarks are extracted :— 
 “The affinity of Owenta to the gravigrade Diprotodons known by their cranial remains 
 is plainly expressed by the structure of its grinding teeth. Had these alone been left 
 to us, it would have been difficult to avoid the error of referring them to a small species 
 of Nototherium. The incisors, on the other hand, are so strongly differentiated, not 
 only from those of Diprotodon, Nototherium, and Sthenomerus, but from those of the 
 phytophagous marsupials generally, that, had these been our sole guides, we might have 
 been led to speculate on the existence of a carnivore more destructive than Thylacoleo ; 
 but its general relationship being evident, it is only necessary to ascertain to which of 
 the older and better known genera it has the nearest alliance. The absence of the 
 dilated muzzle, flat face, elevated forehead, huge zygomata, and strongly inflected 
 mandibular angle of Notutherium, shows that in its leading characters its affinity to 
 that genus was anything but close. From Diprotodon it was not so far removed ; in the 
 several features in which it departs from Nototherium, it approaches --or rather departs 
 
 
 
 *In his Paper on Diprotodon minor Mr. De Vis commits a strange bibliographical error. He quotes 
 as the original reference to this species the ‘‘ Annals and Magazine of Natural History,” vol. xviii., pp. 
 422-427, It should be as above given. 
 
670 
 
 from—its more ponderous contemporary. In the conformation of the posterior 
 
 moiety of the mandible, that of the condyle excepted, it indeed resembles Diprotodon 
 rather closely ; the position of the dental foramen in the two is almost identical, and 
 the chief difference is the relatively greater development of the alar expansion in the 
 newer genus.” 
 
 The premolars are described in general terms as simple unilobate teeth; the 
 upper one subtriangular in section, with the subcentral conical cusps longitudinally 
 constricted towards the apex, the constriction being still seen in a contraction of the 
 dentinal band, as it traverses obliquely the longitudinal axis of the teoth. The lower 
 premolar is structurally the same as in Wototherium, as identified by Owen, therefore 
 the upper one of Wototherium should not differ mridely from that of the present genus, 
 
 In his last communication, Mr. De Vis has wisely changed the name from 
 Owenia to Euowenia, the former having been preoccupied no less than three times—in 
 1847 by Presch for a genus of Cephalopoda; in 1853 by Kollicker for a Colenterate, 
 and, according to Count Marschall, by one of the Agassiz in 1860 for a Ctenophore. 
 
 Loc. and Horizon. Chinchilla, Darling Downs (A. Broadbent—Colln. Queens- 
 land Mus.)—Chinchilla Conglomerate. 
 
 EvoweEnia ropusta, De Vis. 
 Euowenia robusta, De Vis, Proc. Linn. Soc. N. S. Wales, 1891, vi. (2), Pt. 2, p. 160. 
 
 Obs. A second species founded on “ the inferior moiety of the articulating limb 
 with the dentary limb of the left sidein natural conjunction with the anterior half of the 
 dentary limb of the aN, side, all the teeth of the parts preserved being in place csp 
 m.* of the left side. 
 
 This fossil represents avery much more robust animal than Z. grata, with a lower 
 symphysial gradient, a parabolic instead of an angular inferior contour, and compressed 
 rather than rotund incisors. 
 
 Loc. and Horizon. Darling Downs (C. W. De Vis—Colln. Queensland Mus.)-— 
 Fluviatile deposits. 
 
 Family—PHALANGERIDZ. 
 
 Genus—PHALANGER, Storr, 1780. 
 (Prod. Meth. Mam., p. 33.) 
 
 PHALANGER PROCUSCUS, De Vis. 
 Cuscus procuscus, De Vis, Proc. R. Soc. Queensland, 1889, vi., Pts. 2 and 3, p, 111, t. 5, lower right-hand fig. 
 
 Obs. The anthral end of a right scapula has been referred to the genus Phalanger 
 (Cuscus) under the above name, the Author remarking that it ‘ brings us into nearer 
 contemplation of the recent genus Cuscus than was permitted to us by Archizonurus.” 
 Its size was about equal to that of the last-named genus, and its nearest living ally is 
 Phalanger (Cuscus) orientalis, a New Hebridean species. Touching the size of this 
 extinct “ Possum,” the Author remarks—‘ The greatest breadth of the glenoid fossa in 
 the fossil is sixfold that of P. Archeri; its length has nearly the same proportion. LP. 
 Archeri is 310 mm. in length, sine cauda, and weighs aboutfour pounds. <Archizonurus 
 may, therefore, be estimated to have been about six feet in length, and 850 lb. in 
 weight.” . 
 
 Loc and Horizon. Darling Downs (C. W. De Vis—Colln. Queensland Mus.) — 
 Fluviatile deposits. 
 
671 
 
 Genus—PSEUDOCHIRUS, Ogilby, 1836. 
 (Proc. Zool. Soc., 1836, p. 26.) 
 
 PsrvupocHtrus ? NOTABILIS, De Vis. 
 Pseudochirus notabilis, De Vis, Proc. R. Soc. Queensland, 1889, vi., Pts. 2 and 3, p. 118, t. 5, lower left- 
 hand fig. 
 
 Obs. A maxillary with the premolar (pm. 4) and three succeeding molars is 
 referred by Mr. De Vis provisionally to Psewdochirus ‘as the most likely amongst living 
 genera to have been transmitted through it, but at the same time a possible affinity with 
 Cuscus on the one hand and even Phascolarctos on the other is not to be altogether 
 ignored.” P. notabilis is believed to have been as large as a Koala, and would conse- 
 quently weigh about twenty pounds. 
 
 Loe. and Horizon. Darling Downs (C. W. De Vis—Colln. Queensland Mus.)— 
 Fluviatile deposits. 
 
 Genus—KOALEMUS, De Vis, 188S.. 
 (Proc. R. Soc. Queensland, vi., Pts. 2 and 8, p. 106.) 
 
 KoaLemus INGENS, De Vis. 
 Koalemus ingens, De Vis, Proc. R. Soc. Queensland, 1889, vi., Pts. 2 and 3, p. 106, t. 5, up. right-hand fig, 
 
 Obs. This genus and species are founded on the distal end of aright fibula— 
 and there is also provisionally referred to it a premaxillary with its palatal process—of 
 an animal allied to, although not congeneric with Phascolarctos, the Native-bear. 
 
 The fossil bone is said to have a strong general resemblance in form and 
 arrangement of its parts with the corresponding one in the living animai, but the 
 following differences given in the Author’s words may be taken as distinctive :—“ The 
 anterior segment of the epectosphere produced but very slightly at its anterior angle, 
 forming a roughened triangular plane, impinging by the posterior angle upon the side 
 of the posterior segment. The groove segmenting the epectosphere is broadly concave 
 at the base. The shaft subquadrate, flattened on the exterior and anterior sides, which 
 
 * meet on a strong angular ridge continued distal to the anterior segment. Expansion 
 of the shaft, proximal of the epiphysis, very moderate.” 
 
 Mr. De Vis adds that taking the weight of an adult Koala or Native-bear at 
 twenty pounds, that of the extinct form would in comparison ‘be estimated at five 
 hundred-weight or more.” 
 
 Loe. and Horizon. Darling Downs (C. W. De Vis—Colln. Queensland Mus.)— 
 Fluviatile deposits. 
 
 Genus—ARCHIZONURUS, De Vis, 1889. 
 (Proc. R. Soc. Queensland, vi., Pts. 2 and 3, p. 109.) 
 
 ARCHIZONURUS sECURUS, De Vis. 
 Archizonurus securus, De Vis, Proc. R. Soc. Queensland, 1889, vi., Pts. 2 and 3, p. 109, t. 5, up. left- 
 hand fig. 
 
 Obs. An extinct true Phalanger founded on the distal third of a shoulder blade 
 “distinguished by a large dilated and incrassated coracoid, which firmly denies all 
 relationship with families other than the Phalangistide.” In form this bone is hardly 
 to be distinguished from the corresponding one in the Toolah, Phalangista Archeri, but it 
 differs from this and all other Phalangers “in not having its rostral edges brought 
 together and produced at the point into a bicipital tubercle; the external edge is, on 
 the contrary, reflected upon the ectal surface of the bone.” 
 
 Loe. and Horizon. Darling Downs (C. W. De Vis—Colln. Queensland Mus.)— 
 
 Fluyiatile deposits. 
 
672 
 
 Genus—THYLACOLEO, Owen, 1858. 
 (Proc. R. Soce., ix., p. 565.) 
 
 THYLACOLEO CARNIFEX, Owen. 
 
 Thylacoleo carnifex, Owen, Phil. Trans., 1859, cxlix., p. 309, t. 11, f. 1-6, t. 18, f. 1, 4-8, t. 14, f. 1, t. 15, f 15 
 Ibid., 1866, clvi., Pt.1, p. 73, t. 2, 3,and4; Zbid., 1871, clxi., Pt. 1, p. 213, t. 11, 
 12, 13, and 14; Jbid., 1883, clxxiv., Pt. 2, p. 575, t. 39, 40, and 41, f. 1 and 2, 
 p. 639, t. 46, f. 1. 
 ys 2 Owen, Extinct Mam. Australia, 1877, p. 107, t. 6, f. 1, 6, 9, 10, and 12, t. 7, f. 1-14, t. 
 8, f..1-6, 11 and 13, t. 9, f. 1-9, t. 10, t. 11, t. 13, £. 1, 4-8, t. 14, £. 1, t. 15, f. 1, 6. 
 16, 17, and 18. 
 » 0 Owen, Geol. Mag., 1883, x., p. 289, t. 7. 
 Obs. The sectorial teeth of this species demonstrate the presence, during Post- 
 Tertiary times, of a large Carnivore, the marsupial character of which is indicated by 
 the name “‘ Marsupial or Pouched Lion.” The dental formula is 7. 22, c. +4, p. #4 
 
 0-0? P- 4-4) 
 Mm. i= 30. 
 
 Mr. C. W. De Vis has lately described * a femur, believed by him to be that of 
 Thylacoleo, from the Darling Downs. He remarks—‘‘The bone is in general form 
 unlike any recent femur known to the Writer, inasmuch as it tapers gradually from 
 the proximal end to the distal third-fifth, and is in its proximal moiety rather strongly 
 curved, both inwards and outwards.” Again—“‘ The fossil resembles the femur 
 of the Carnivore in the shortness and direction of the lesser trochanterian ridge, 
 in the obliquity of the post trochanterian fossa, in the shape of the head, 
 in that of the shaft anteriorly, and generally of the whole distal extremity. To 
 this we may add that the backward curvature of the shaft is found in the allied genus 
 Dasyurus. On the other hand, it resembles the corresponding bone in Phascolomys in the 
 shape of the great trochanter exteriorly, in the prominence of the lesser trochanter, in the 
 insertion of the ligamentum teres, in the depth of the neck between the great trochanter 
 and the head, and in the turgidity of the space between the fossa and the head. In brief, 
 its proximal extremity, with prevailing characters of its own, has more of Phascolomys 
 than of Sarcophilus in its composition, while its shaft and distal end show relation almost * 
 exclusively (as between these two) to Sarcophilus. But withal there are features of 
 Macropus not to be overlooked: the angle of articulation, the shape anteriorly and length 
 of the outer condyle, the tumid quadratus insertion, and the extra-condylar groove. 
 ‘We may sum up the whole by saying that sarcophiline affinities are dominant, phas- 
 colomine subordinate, macropine concomitant.” 
 
 Loc. and Horizon. Gowrie, Darling Downs (S. St. Jean) ; Hodgson’s Creek, 
 Darling Downs (The late 8. Strutchbury) ; Eton Vale, Darling Downs (£. 8. Hill) ; 
 King’s Creek, Darling Downs (The late C. H. Hartmann)—Fluviatile deposits. 
 
 Family—MACROPODIDA. 
 
 Genus—MACROPUS, Shaw, 1800. 
 (Gen. Zoology, i, Pt. 2, p. 505.) 
 
 Obs. ihroaetout this family I have, as far as possible, adopted the subdivisions 
 proposed by Prof. Owen, and his references ; but, for the sake of convenience, the sub- 
 genera are treated as genera. This does not altogether accord with Mr. Lydekker’s 
 arrangement in the British Museum “ Catalogue of Fossil Mammalia,” Part 5, where 
 Leptosiagon, Pachysiagon, Osphranter, Phascolagus, and in part Protemnodon and 
 
 * On a Femur, probably of Zhylacoleo. Proc. R. Soc. Queensland, 1886, iii., p. 122, t. 3. 
 
673 
 
 Sthenurus, are merged in Macropus. The greater portion of this section of the present 
 work was compiled before the appearance of the British Museum Catalogue, and to this 
 the reader is referred for the unravelling of the intricate synonymy attached to these 
 fossils. The fossil Macropodide have recently been re-studied by Mr. De Vis in the 
 light thrown on them by the very large Collection in the Queensland Museum, but the 
 results await publication. 
 Macrorvs TITAN, Owen. 
 Macropus titan, Owen, in Mitchell, Three Expeds. Int. E. Australia, 1838, ii., p. 359, t. 29, f. 3, 6, and 8. 
 
 “A », Owen, Descrip. Cat. Mam. Aves R. Col. Surgeons, 1845, p. 324, Nos. 1510-12, 1526, 1528- 
 boy ta Gate te 
 * ,» Phil. Trans., 1874, clxiv., Pt. 1, p. 248, t. 20, £. 29, t. 21, f. 6-18, t. 22, f. 10-18, t. 23, f. 2 
 
 and 3, 12 and 13, t. 26, f. 9-15; Ibid., 1874, Pt. 2, p. 783, t. 76, £. 1-6; Ibid., 1876, 
 elxvi., Pt. 1, p. 204, t. 25, £. 1 and-4, t. 26, f. 1 and 2, t. 27. 
 
 “6 », Owen, Extinct Mam. Australia, 1877, pp. 400, 435, 489, 499, t. 76, f. l and 4, t. 77, f. 1 
 and 2, t. 79, f.1 and 2, t. 80, f. 29, t. 81, f. 6-18, t. 82, f. 10-18, t. 83, f. 2 and 3, 12 
 and 13, t. 86, f. 9-15, t. 69, £. 1-6, t. 112 and 113, t. 118, f. 1-7. 
 
 a », Etheridge fil., Cat. Australian Foss., 1878, p. 183 (for full synonymy). 
 
 A »» Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 225. 
 
 Obs. The former existence of this species was determined by Prof. Owen upon 
 the evidence afforded by portions of several jaws and a humerus, &c., obtained from the 
 Wellington Valley Caves and the Queensland Freshwater deposits. The remains 
 exceeded in size those of the living Macropus major. The humerus exceeds in length 
 that of the last-named species as much as that of Phascolagus falls short of it, and the 
 strength or thickness of this bone is greater than in the latter. 
 
 In addition to these remains, a very fine skull, more or less complete, was 
 obtained by Mr. W. F. Tooth, Junr., at King’s Creek, Darling Downs, the measurements 
 of which, as compared with a skull of Macropus major, are given by Sir R. Owen.* 
 
 Macropus titan is closely allied to the living IZ. giganteus, “ but is distinguished by 
 its superior size, and the very general occurrence of one or more vertical grooves on the 
 hinder surfaces of the lower true molars; it is, however, probable that the two forms 
 pass imperceptibly into one another.” 
 
 Loc. and Horizon. Condamine River, west of Moreton Bay (Sir 7. L. Mitchell— 
 Colln. College of Surgeons, London); Darling Downs (H. Hughes—Colln. Worcester 
 Nat. Hist. Soc.); Darling Downs (Sir C. Nicholson—Colln. Oxford Museum); Gowrie, 
 Darling Downs (Dr. G. Bennett) ; King’s Creek, Darling Downs (W. F. Tooth, Junr., 
 and Dr. G. Bennett)—Fluviatile deposits; Maryvale Creek, Clarke River (The late 
 R. Daintree)—Diprotodon-breccia. 
 
 MAcROPUS AFFINIS, Owen. 
 Macropus affinis, Owen, Descrip. Cat. Mam. Aves. R. Coll. Surgeons, 1845, p. 328, No. 1524. 
 
 ry! » Owen, Phil. Trans., 1874, clxiv., Pt. 1, p. 260, t. 23, f. 10 and 11; Zbd., 1876, clxvi., Pt. 1, 
 p. 217, t. 29; £. 6, t. 30, £. 7-9. 
 
 ay », Owen, Extinct Mam. Australia, 1877, pp. 411 and 498, t. 83, f. 10 and 11, t. 116, f. 6, 
 Gal l'7,fap7-9, 
 
 PP », Etheridge fil, Cat. Australian Foss., 1878, p. 183 (for full synonymy). 
 
 Obs. Under this name Sir R. Owen described a left mandibular ramus with 
 teeth, indicating a species of less size than Macropus titan. He remarks—“ Evidence of 
 an extinct Kangaroo of intermediate proportions between the largest known living 
 species and those defined in my original Memoirs.” + 
 
 Loc. and Horizon. Condamine River, west of Moreton Bay (Sir 7. L. Mitchell— 
 
 Colln. College of Surgeons, London); King’s Creek, Darling Downs (G. F. Bennett)— 
 Fluviatile deposits. 
 
 * Extinct Mam. Australia, 1877, p. 436. 
 
 + Phil. Trans., 1874, clxiv., Pt. 1, p. 260. 
 27 
 
674 
 
 Macrorus asax, Owen. 
 Macropus ajax, Owen, Quart. Journ. Geol. Soc., 1859, xv., p. 185, note. 
 Obs. This name was applied to a lower jaw which does not appear to have been 
 referred to. in any of Prof. Owen’s subsequent Memoirs. 
 Loe. and Horizon. Darling Downs (H. Hughes—Colln. Worcester Nat, Hist 
 Soc.) —F luviatile deposits. 
 Macropus ropustvus, Gould. 
 
 Petrogale robusta, Gould, Mon. Macropodide, 1841, t. 5. 
 Osphranter robustus, Gray, List Spec. Mam. Brit. Mus., 1843, p. 91. 
 Macropus robustus, Lydekker, Cat. Foss. Mam. Brit. Mus., Pt. 5, 1887, p, 222. 
 
 Loc. and Horizon. Gowrie, Darling Downs (@. F. Bennett—Colln. Brit. Mus.) 
 
 —Fluviatile deposits. 
 Macrorvs, sp. tnd. (a). 
 Macropus, sp., Owen, Descrip. Cat. Mam. Aves. R. Coll. Surgeons, 1845, p. 326, No, 1517. 
 
 Obs. A ramus of a lower jaw was retained by Prof. Owen in the Royal 
 College of Surgeons Catalogue as a distinct species. It presented evidence of more 
 molars in use at one time than in the recent Macropus laniger or M. major. 
 
 Loe. and Horizon. Condamine River, west of Moreton Bay (Sir Z. L. Mitchell 
 —Colln. College Surgeons, London) —F luviatile deposits. 
 
 Macropvs, sp. ind. (0). 
 Macropus, sp., Owen, Extinct Mam. Australia, 1877, p. 491, t. 114. 
 Obs. An almost entire femur has been described by Sir R. Owen, and does not 
 appear referable to any described species. 
 Loc, and Horizon. King’s Creek, Darling Downs—Fluviatile deposits. 
 
 Genus—LEPTOSITAGON, Owen, 1873. 
 (Proc. Roy. Soc., xxi., p. 386.) 
 
 LEPTOSIAGON GRACILIS, Owen. 
 
 Leptosiagon gracilis, Owen, Proc. R. Soc., 1873, xxi., p. 386. 
 oF uA Owen, Phil. Trans., 1874, clxiv., Pt. 2, p. 785, t. 76, f. 11-15. 
 . +5 Owen, Extinct Mam. Australia, 1877, p. 450, t. 89, f. 11-15. 
 
 Obs. Prof. Owen considers Leptosiagon to be a sub-genus of Macropus. He 
 adds—“ The distinctive dental character of the present sub-genus is in the sculpturing 
 of the hind surface of the molars,” and the mandible appears to have been unusually thin 
 in proportion to its depth. Mr. Lydekker remarks that the specimen on which this 
 species was founded presents no distinguishable difference from Macropus (Pachysiagon) 
 ferragus, Owen.* 
 
 Loe. and Horizon. The only locality afforded is that of “ Queensland.’”’ Probably 
 from Darling Downs.—Fluviatile deposits. 
 
 Genus—OSPHRANTER, Gould, 1841. 
 (Proc. Zool. Soc., Pt. ix., p. 80.) 
 
 OsPHRANTER COOPERI, Owen. 
 Osphranter Cooperi, Owen, Proc. R. Soc., 1873, xxi., p. 128. 
 * = 5) hil. Trans., 1874, clxiv., Pt. 1, p. 261;.t. 24,4. 17 and 18; 
 »> Extinct Mam. Atstealin: 1877, p. 412, t. 84, f. 17 and 18, 
 Heo Conn Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 234. 
 
 Obs. This name was applied by Prof. Owen to the “fore part of the left man- 
 dibular ramus of an aged individual of a Wallaroo, of the size of Osphranter robustus.” 
 Loc. and Horizon. Darling Downs, Queensland—Fluviatile deposits. 
 
 * Cat, Foss, Mam. Brit. Mus., 1887, Pt. 5, p. 231. 
 
 
 
 
 
675 
 
 OsPHRANTER GOULDII, Owen. 
 
 Osphranter Gouldii, Owen, Proc. R. Soc., 1873, xxi., p. 128. 
 of .; Phil. Trans., 1874, clxiv., Pt. 1, p. 261, t. xxiii., f. 15 and 16, 
 os - Extinct Mam. Australia, 1877, p. 418, t. 83, f. 15 and 16. 
 
 Obs. A corresponding but smaller species of Wallaroo than the last. The name 
 was also founded on the left mandibular ramus. Mr. Lydekker refers this to the living 
 Macropus Parryi, Bennett.* . 
 
 Loc. and Horizon. Darling Downs.—Fluviatile deposits. 
 
 Genus—PALORCHESTES, Owen, 1873. 
 (Proc. R. Soc., xxi., p. 386; Phil. Trans., 1874, clxiv., Pt. 2, p. 797.) 
 
 PALORCHESTES AZAEL, Owen. 
 
 Palorchestes azael, Owen, Phil. Trans., 1874, clxiv., Pt. 2, p. 798, t. 81, f. l and 2, t. 82, f. 1 and 2, t. 83, f. 
 1; Ibid., 1876, clxvi., Pt. 1, p. 197, t. 19-21, t. 22, f. 1-4, t, 23, f.1, 2, and 5, t. 24, 
 t. 29, f. 1-3. 
 Owen, Extinct Mam. Australia, 1877, pp. 466 and 500, t. 96, f. 1 and 2, t. 97, f. 1 and 2, 
 t. 105, f. 1, t. 106 and 107, t. 115, f. 1, 2, and 5, t. 116, f. 1-3, t. 129, t. 130, f. 1-4, t. 131. 
 De Vis, Proc. Linn. Soc. N.S. Wales, 1883, vili., Pt. 2, p. 221. 
 “ “r Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 237. 
 
 Obs. Portions of jaws were described by Sir R. Owen, under this name, without 
 assigning to them any definite locality. He considers that these remains deviate less 
 from the type of the bilophodont Macropodide. than those of Procoptodon, some of 
 which, P. Goliah, for example, were of larger bulk. The entire skull would probably 
 measure about sixteen inches in length. 
 
 Mr. De Vis has described a portion of the jaw and dentition, since the appearance 
 of Owen’s “ Extinct Mammals of Australia.” He considers P. azael to have been a 
 true saltigrade of Macropodoid type. 
 
 Loc. and Horizon. Near St. Ruth, Darling Downs, at a depth of seventy feet 
 from the surface (C. W. De Vis—Colln. Queensland Mus.)—Fluviatile deposits. 
 
 > ” 
 
 ” ”? 
 
 Genus—PACHYSIAGON, Owen, 1873. 
 (Proc. R. Soc., xxi., p. 386.) 
 
 Obs. This name was applied by Sir R. Owen to two extinct species of 
 Macropodide in which the massiveness of the mandible was greatly in excess of the 
 
 teeth it supported. 
 PACHYSIAGON FHERRAGUS, Owen. 
 
 Macropus Ferragus, Owen, Phil. Trans., 1874, clxiv., Pt. 2, p. 784, t. 81, f. 4, t. 82, f. 3 and 4, t. 105, f 3. 
 Pachysiagon Ferragus, Owen, Extinct Mam. Australia, 1877, p. 449, t. 96, f. 4, t. 97, f. 3 and 4, t. 105, f. 3. 
 
 Obs. <A portion of right mandibular ramus indicated to Prof. Owen, by the size 
 of the teeth and the jaw itself, a Kangaroo exceeding in size the Macropus titan. Mr. 
 Lydekker refers this species to Macropus, and unites with it Leptosiagon gracilis, Owen. 
 
 Loc. and Horizon. Condamine River, Darling Downs (Colln. Brit. Mus.)— 
 
 Fluviatile deposits. 
 PACHYSIAGON OTUEL, Owen. 
 
 _Pachysiagon otuel, Owen, Phil. Trans., 1874, clxiv., Pt. 2, p. 784, t. 76, f. 7-10. 
 Procoptodon otuel, Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 236. 
 
 Obs. This species is said to show the typical generic characters in a more marked 
 manner than P. ferragus. 
 
 
 
 * Cat. Foss, Mam, Brit. Mus., 1887, Pt. 5, p, 220, 
 
676 
 
 Loc. and Horizon. King’s Creek, Darling Downs (G. B. King—Colln. Brit. 
 Mus.)—Fluviatile deposits. 
 
 Genus—P HASCOLAGUS, Owen, 1873. 
 (Proc. R. Soc., xxi., p. 128; Phil. Trans., 1874, clxiv., Pt. 1, p. 261.) 
 
 PHASCOLAGUS ALTUS, Owen. 
 
 Macropus titan, Owen, in Mitchell Three Expeds. Int. E. Australia, 1838, ii., t. 29, f. 4 and 5 (excl. 
 f, 3, 6, and 8). 
 Phascolagus altus, Owen, Phil. Trans., 1874, clxiv., Pt. 1, p. 261, t. 22, f. 1 and 2; Jbid., 1876, clxvi., Pt. 1, 
 p. 218, t. 30, f. 1-6. 
 », Owen, Extinct Man: Australia, 1877, pp. 414 and 498, t. 82, f. 1 and 2, t. 117, f. 1-6, 
 Maoropus altus, Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 223. 
 
 Obs. Of this species Sir R. Owen has described a right maxillary with teeth, 
 and a metatarsal. Teeth of the molar series are equal in extent and size to those of 
 Macropus rufus and M. major. The pattern of the grinding surfaces of the upper 
 molars is more like that in Halmaturus and Osphranter than in either Macropus major 
 or WM. titan. 
 
 Loc. and Horizon. King’s Creek, Darling Downs (Dr. G. Bennett)—Fluviatile 
 deposits. 
 
 Genus—PROCOPTODON, Owen, 1873. 
 (Proc, R. Soc., xxi., p. 886 ; Phil. Trans., 1874, clxiv., Pt. 2, p. 786.) 
 
 PROCOPTODON PUSIO, Owen. 
 
 Procoptodon. pusio, Owen, Phil. Trans., 1874, clxiv., Pt. 2, p. 788, t: 77, f. 2-7; Ibid., 1876, clxvi., Pt. 1, 
 p. 222, t. 31, f. 1-5, 10-12. 
 5 » Owen, Extinct Mam. Australia, 1877, p. 454, t. 89, £. 7-10, t. 90, f. 2-7, t. 91, t. 119, 
 f, 1-5, 10-12. 
 
 Obs. The remains of this species, examined by Prof. Owen, consisting of jaws 
 with teeth, a metatarsal, &c., indicated a Kangaroo one-third larger than Osphranter 
 robustus, Gould. 
 
 A large unossified tract of the palate, which is shown in both maxillaries of this 
 genus, is not present in the large existing Kangaroos of the genera Macropus and 
 Osphranter. It is present, adds Prof. Owen, under some modifications, in Boriogale, 
 Halmaturus, and Petrogale,and such similar small Kangaroos and Wallabies. 
 
 Loc. The former is not stated, but probably Darling Downs—Fluviatile deposits. 
 
 PROCOPTODON GOLIAH, Owen. 
 
 Macropus goliah, Owen, in Waterhouse, Nat. Hist. Mam., 1846, i., p. 59. 
 Procoptodon goliah, Owen, Phil. Trans., 1874, clxiv., Pt. 2, p. 791, t. 79, t. 80; Ibid., 1876, clxvi., Pt. , 
 p. 222, t. 22, £. 5, t. 23, f. 3and 4, 
 
 A ‘ Owen, Extinct Mam. Australia, 1877, p. 454, f. 89, f. 7-10, t. 90, f. 2-7, t. 91, t. 119, 
 f. 1-5, 10-12. 
 33 * Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 235.~ 
 
 Obs. The portions of this Kangaroo hitherto obtained consist of parts of 
 jaws, of a hind foot, and a left femur. 
 
 Loc. and Horizon. Darling Downs, at a depth of forty feet from the surfaco— 
 (Colln. College of Surgeons, London; Colln, Brit. Mus.; Colln, Australian Mus.)— 
 Fluviatile deposits. 
 
677 
 
 PROCOPTODON RAPHA, Owen. 
 
 Procoptodon Rapha, Owen, Phil. Trans., 1874, clxiv., Pt. 2, p. 788, t. 77, £. 8-12, t. 78; Ibid., 1876, elxvi., 
 p. 222, t. 31, f. 6-9. 
 ” ¥3 Owen, Extinct Mam. Australia, 1877, pp. 457, 483, 494, 502, t. 90, f. 8-12, t. 93, 
 t, 119, f. 6-9, t. 128, 
 > 
 Obs. P.vrapha, from the portions hitherto found, consisting of a lower Jaw, 
 femur, metatarsals, &c., would appear to be of larger size than P. pusio, but inferior to 
 P. goliah. The characters of the jaw are nearer to those of Wototheriwm than 1s 
 usually shown in Macropodoid genera. 
 Loc. and Horizon. Gowrie, Darling Downs (@. F. Bennett)—Fluviatile deposits. 
 
 Genus—PROTEMNOD ON, Owen, 1873. 
 Proc. R. Soc., 1873, xxi., p. 128 ; Phil. Trans., 1874, clxiv., Pt. 1, p. 274.) 
 
 Obs. Protemnodon is allied to Sthenurus, but is distinguished by the “more 
 simple trenchant shape of the crown of the premolars.”” The upper molars are more 
 like those of Sthenurus atlas than those of Macropus titan. 
 
 PROTEMNODON ANAK, Owen. 
 Macropus atlas, Owen, Descrip. Cat. Mam. Aves. R. Coll. Surgeons, 1845, pp. 325 and 327, Nos, 1513 and 
 
 1519. 
 Protemnodon anak, Owen, Phil. Trans., 1874, clxiv., Pt. 1, p. 275, t. 28, f. 4-9, f. 1-4, 7-10, and 14. 
 sc », Owen, Extinct Mam. Australia, 1877, pp. 428, 449, 498, t. 83, f. 4-9, t. 85, f. 1-4, 
 
 7-10, and 14, t. 120, f. 1-6. 
 
 Obs. The remains of this old Kangaroo hitherto found consist of a lower jaw, 
 metatarsal, and other smaller bones. 
 
 Loc. and Horizon. Condamine River, West of Moreton Bay (Sir 7. L. Mitchell 
 —Colln. Coll. Surgeons, London) ; Darling Downs (—. Hughes—Colln. Worcester Nat. 
 Hist. Soe.) ; Eton Vale, Darling Downs (Z. 8. Hill—Colln. Brit. Mus.)—Fluviatile 
 deposits. 
 
 PROTEMNODON ANTHUS, Owen. 
 Protemnodon Anteus, Owen, Extinct. Mam. Australia, 1877, p. 448, t. 88, f. 18, t. 110. 
 
 Obs.- The remains of this species, consisting of a right and left mandibular 
 ramus, with molar dentition, are described by Sir R. Owen without affixing a locality. 
 
 This is united by Mr. Lydekker with Protemnodon rechus, Owen, and referred 
 to Macropus. : 
 
 Loe. and Horizon. Clifton, Darling Downs (Dr. G. Bennett and PF. N. Lsaacs— 
 Colln. Brit. Mus.) ; Gowrie, Darling Downs (Dr. G. Bennett—Colln. Brit. Mus.)— 
 Fluviatile deposits. 
 
 PROTEMNODON MIMAS, Owen. 
 Protemnodon mimas, Owen, Phil. Trans., 1874, clxiv., Pt. 1, p. 278, t. 24, f. 18-16, t. 26, f. 1-8, t. 27, f. 1-4 
 and 14. 
 Fp An Owen, Extinct Mam. Australia, 1877, pp. 431, 447, t. 84, f. 13-16, t. 86, f. 1-8, t. 87, 
 f, 1-4 and 14. ; 
 
 Obs. In this species, says Professor Owen, “a greater depth and thickness of 
 mandible, and a concomitant large size of molars, are associated witha relatively smaller 
 size of the trenchant premolar, which does not exceed that in P. anak.” 
 
 This is united by Mr. Lydekker with Sthenurus brehus, Owen, and referred to 
 Macropus. . 
 
 ; Loc. and Horizon. Gowrie Creek, Darling Downs (Dr. G. Bennett); Eton 
 Vale, Darling Downs (Sir D. Oooper—Colln. Brit. Mus.)—Fluviatile deposits. 
 
678 
 
 Protemnopon Oc, Owen. 
 
 Protemnodon Og, Owen, Phil. Trans., 1874, clxiv., Pt. 1, p. 277, t. 25, f. 5 and 6, 11-18, 
 as », Owen, Extinct Mam. Australia, 1877, p. 480, t.85, f. 5 and 6, 11-18. 
 
 Obs. Of this species Prof. Owen remarks—“ With a certain increase of size 
 of» both mandible and molar teeth, represents the form and size of the premolars in 
 P. Anak.” 
 
 Mr. Lydekker unites the specimens with Protemnodon anak, Owen, in part, and 
 Sthenurus atlas, Owen, in part, and refers them to Macropus. 
 
 Loe. and Horizon. Gowrie, Darling Downs (Sir D. Cooper—Colln. Brit. 
 Mus.)—Fluviatile deposits. 
 
 PROTEMNODON RECHUS, Owen. 
 
 Protemnodon rechus, Owen, Phil. Trans., 1874, clxiv., Pt. 1, p. 281, t. 27, f. 10-13. 
 ” »» Owen, Extinct Mam, Australia, 1877, p. 434, t. 87, f. 10-13. 
 
 Obs. In a left mandibular ramus “the molars have the characters of those of 
 P.anak . . . but the increase in size is more than can be granted to difference 
 of sex.’’ 
 
 Loc. and Horizon. King’s Creek, Clifton Station, Darling Downs (@. King)— 
 Fluviatile deposits. 
 
 Genus—STHENURUS, Owen, 1873. 
 (Proc. R. Soc., xxi., p. 128.) 
 
 STHENURUS ATLAS, Owen. 
 
 Macropus Atlas, Owen, in Mitchell Three Expeds. Int. E. Australia, 1838, ii., p. 359, t. 29, f. 1. 
 
 Owen, Descrip. Cat. Mam. Aves R. Coll. Surgeons, 1845, pp. 325-330, Nos. 1513-16, 1519- 
 1520, 1525, and ? 1527. 
 
 Sthenurus atlas, Owen, Phil. Trans., 1874, clxiv., p. 265, t. 20, f. 30, t. 22, f. 3-9, t. 24, £. 4-93 Jbid., 1876, 
 clxvi., Pt. 1, p. 210. 
 
 Owen, Extinct Mam. Australia, 1877, pp. 416, 439, 446, t. 76, f. 2 and 3, t. 77, f. 4 and 5, 
 t. 79, £. 4, t. 80, f. 30, t. 82, £. 3-9, t. 84, £. 4-9, t. 88, f. 1-4. 
 
 Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 232. 
 
 ” 99 
 
 Obs. The form and structure of the premolars in this and its fellow species, as 
 compared with their proportion to the molars behind, indicate, according to Prof. Owen, a 
 distinct sub-genus of Macropodide. The name Sthenurus was suggested by the form 
 and proportions of the vertebre of the very powerful tail of this great extinct Kangaroo. 
 The portions hitherto recorded consist of jaws with teeth, portion of a skull, and tail 
 vertebra. 
 
 Loc. and Horizon. Darling Downs (Sir C. Nicholson—Colln. Oxford University 
 Mus.) ; Gowrie, Darling Downs (Sir D. Cooper—Colln. Brit. Mus.)—Fluviatile deposits. 
 
 STHENURUS BREHUS, Owen. 
 
 Sthenurus Brehus, Owen, Phil. Trans., 1874, clxiv., Pt. 1, p. 272, t. 27, £.5-9 ; Ibid., 1876, clxvi., Pt.1, p. 212, 
 t. 28. 
 = as Owen, Extinct Mam. Australia, 1877, pp. 424, 442, 449, t. 87, f. 5-9, t. 88, f. 5-10,t. 92, 
 f. 6 and 7, t. 108, t. 109, ? t. 77, £.-7. 
 Macropus brehus, Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 207. 
 
 Obs. The foremost of the upper incisors in this species “has a greater relative 
 superiority of size over the second and third than in any existing species of Kangaroo.” 
 Loc. and Horizon. Clifton Station, Darling Downs.—F luviatile deposits. 
 
679 
 
 Genus—STHENOMERUS, De Vis, 1883. 
 (Proc. Linn. Soc. N. S. Wales, viii., Pt. 1, p. 15.) 
 
 STHENOMERUS CHARON, De Vis. 
 Beinerié Charon, De Vis, Loe. cit., p. 15. 
 
 Obs. Of this animal the portions hitherto discovered consist of a deciduous 
 molar, a femur, radius, and ulna. Mr. De Vis remarks—‘ In dentition the animal 
 diverges considerably from Wototheriwm, more so from Diprotodon ; its divergence is 
 towards the Macropodide. In its long bones it approaches very closely to Diprotodon, 
 possibly to Nototherium also. Its thigh-bone shows that it hardly departed from these 
 in the structure and movements of its hind-quarters. It is, in sbort, a transition form.” 
 
 The tooth is fourteen lines in length, ten and a-half lines in its anterior and 
 nine lines in its posterior transverse diameter. 
 
 Loc. and Horizon. Gowrie Creek, Darling Downs (H. Tryon—Colln. Queens- 
 land Mus.)—Fluviatile deposits. 
 
 Genus—BRACHALLETES, De Vis, 18838. 
 (Proc. Linn, Soc. N. S. Wales, vili., Pt. 3, p. 191.) 
 
 BRACHALLETES PatmEnt, De Vis. 
 Brachalletes Palmeri, De Vis, Loc. cit., p. 191. 
 
 Obs. Mr. De Vis has lately drawn attention to the great divergence which 
 exists amongst the various genera of Macropodide in the “gluteal angle” of the 
 femur. “ By gluteal angle is meant the angle made with the long axis of the bone by 
 a straight line touching the top of the trochanter and the summit of the head”’ of the 
 bone in question. The value of this angle, adds Mr. De Vis, expresses the measure of 
 the leaping ability of the animal. 
 
 A femur lately discovered, having the very open gluteal angle of 773°, has 
 afforded this Author the opportunity of establishing the above genus, the loss of 
 saltatory power consequent on this open angle quite precluding its reference to any of 
 the more typical genera of Macropodide. The femur of B. Palmert was equal in size 
 to that of Palorchestes azael, Owen, and not much inferior to Procoptodon goliah, 
 Owen. The generic name has reference to the contracted gait of the animal. 
 
 Loc. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queers 
 land Mus.)—Chinchilla Conglomerate. 
 
 Genus—TRICLIS, De Vis, 1888. 
 (Proc. Linn. Soc. N. S. Wales, iii. (2), Pt. 1, p. 8.) 
 
 TRICLIS OSCILLANS, De Vis. 
 Triclis oscillans, De Vis, Loe. cit., p. 8, t. 1. 
 
 Obs. Both genus and species are founded on a left mandibular ramus, which 
 seems to indicate an animal allied to a gigantic Hypsiprymnodon. Mr. De Vis remarks :— 
 “Tt would seem that the relations of the extinct animal are complex ; capriciously, as it 
 were, its relic yields us glimpses of each of the three families so frequently named 
 [z.e., Phalangeride, Pleopodide, and Macropodide] . . . . . Though its affinity 
 to Hypsiprymnodon may be said to be paramount, it must be confessed that it is not so 
 to any great extent.” 
 
 In Triclis the lower incisor is followed by a tooth, small in size, but occupying 
 the position of the so-called canine in the Phalangeride. In Hypsiprymnodon, on the 
 other hand, this tooth is absent. 
 
680 
 
 The name Triclis had already been employed by Loew for a genus of Diptera, in 
 1851. 
 
 Loc. and Horizon. King’s Creek, Darling Downs (2. Frost—Colln. Queensland 
 Mus.)—Fluviatile deposits. 
 
 Genus—SYNAPTODON, De Vis, 1889. 
 (Proc. R. Soc. Queensland, v., Part 5, p. 159.) 
 
 Gen. Char. Molars rooted, antibilophodont, distant at base, in contact by 
 facetted projections fore and aft. (De Vis.) 
 
 Obs. This genus is founded on a fragment of a right lower jaw, says Mr. De 
 Vis, with a nearly perfect cheek-tooth and the half of its adjacent posterior neighbour, 
 which are said in their form and connection to be unique. They abut against each other, 
 not by a basal line of contact, resulting from pressure in the rear as usual, but by means 
 of coadapted processes extending from each end of each tooth, somewhat after the 
 fashion of a vertebral zygopophysis. . 
 
 SYNAPTODON HyoruM, De Vis. 
 Synaptodon cevorum, De Vis, Proc. R. Soc. Queensland, 1889, v., Pt. 5, p. 169. ; 
 Sp. Char. The perfect tooth is nine millimetres in length, and five millimetres 
 
 in its greatest breadth. The space between the teeth is nearly equal to the length of 
 each fore lobe. (De Vis.) 
 
 Obs. The general facies of the teeth induced the Author above quoted to con- 
 sider them as belonging to a new genus of Macropodide. 
 
 Loe. and Horizon. Chinchilla, Darling Downs—(Colln. Queensland Mus.)— 
 Chinchilla Conglomerate. 
 
 Family—DASYURIDZ&. 
 
 Genus—THYLACINUS, Temminck, 1827. 
 (Mon. Mammologie, i., p. 60.) 
 
 THYLACINUS SPELHUS, Owen. 
 
 Dasyurus laniarus (pars.), Owen in Mitchell Three Exped. Int. E. Australia, 1888, ii., p. 363, t. 31, f. 7. 
 Thylacinus spelceus, Owen, Descrip. Cat. Mam. and Aves R. Coll. Surgeons, 1845, pp. 335-36, Nos. 1548-49. 
 s5 major, Owen, Extinct Mam. Australia, 1877, p. 106. 
 ie »,  Luydekker, Cat. Foss, Mam. Brit. Mus., 1887, Pt. 5, p. 264. 
 
 Obs. This species is said to be represented from the Queensland Post-Tertiary 
 Series by part of aright ulna, and axis vertebra in the British Museum (Natural 
 History Branch). 
 
 Loc. and Horizon. Queensland (Colln. Brit. Mus.)—Fluviatile deposits. 
 
 Genus—SARCOPHILUS, F. Cuvier, 1838. 
 (Hist. Nat. Mam., vii., 70me Livr., p. 2.) 
 
 SARCOPHILUS LANIARIUS, Owen. 
 
 Dasyurus laniarius, Owen in Mitchell Three Exped. Int. E. Australia, 1838, ii., p. 363, t. 31, f. 3-6. 
 Sarcophilus laniarius, Owen, Extinct Mam. Australia, 1877, p. 105, t. 5, f. 1-6. 
 a a Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 265. 
 
 Loc. and Horizon. Gowrie, Darling Downs (G. F. Bennett—Colln. Brit. Mus.) 
 —Fluviatile deposits. 
 
681 
 
 SARCOPHILUS PRIOR, De Vis. 
 Sarcophilus prior, De Vis, Proc. Linn. Soc. N. S. Wales, 1883, viii., Pt. 2, p. 189. 
 
 Obs. The discovery of a portion of a right tibia, with the head preserved, has 
 enabled Mr. De Vis to determine the former presence in Northern Australia of an 
 animal allied to the Tasmanian Devil. The bone gives the impression of a better-knit 
 and more muscular animal, of a size too superior to be included in the same species 
 with §. wrsinus, one whose last molar must have equalled, or nearly equalled in size, the 
 great sectorial of a large dog. 
 
 Loc. and Horizon. Darling Downs (C. W. De Vis—Colln. Queensland Mus.)— 
 Fluviatile deposits. 
 
 Genus—DASYURUS, Geoffroy, 1796. 
 si (Bull. Soc. Phil. Paris, i., p. 106.) 
 
 Dasyurus viverrinus, Shaw. 
 
 Didelphis viverrinus, Shaw, Gen. Zool., 1800, i., Pt. 2, p. 433. 
 Dasyurus viverrinus, Waterhouse, Nat. Hist. Mam., 1846, i., p. 442. 
 + A Krefft, Mam. Australia, 1871, t. 13. 
 9 of Lydekker, Cat. Foss. Mam. Brit. Mus., 1887, Pt. 5, p. 268. 
 
 Obs. Numerous fragments of the skeleton ofthe Native Cat have been found 
 in the Wellington Valley Caves, but only one specimen, a nearly entire right mandibular 
 ramus, has been recorded from Queensland. 
 
 | Loe. and Horizon. Gowrie, Darling Downs (G. F. Bennett-—Colln. Brit. Mus.) 
 —Fluviatile deposits. 
 
 MARSUPIALIA INCERTA SEDIS. 
 
 Genus—SCHPARNODON, Ramsay. 
 (Proc. Linn. Soc. N. 8. Wales, 1881, v., Pt. 4, p. 495.) 
 
 Sceparnopon Ramsay, Owen. 
 Sceparnodon Ramsayt, Owen, Phil. Trans., 1884, clxxv., Pt. 1, p. 245, t. 12. 
 
 Obs. But one species of this genus, and of that only the teeth are known. They 
 resemble the scalpriform incisors of the upper jaw of Rodents, but the microscopic 
 structure of the dentine has a nearer resemblance to that of the incisors of the large 
 extinct Phascolonus. 
 
 Sceparnodon Ramsayi is believed by Prof. Owen to have been a large massive 
 animal, and in all probability matsupial. Mr. Richard Lydekker has recently suggested* 
 that it is identical with Owen’s genus Phascolonus ; but Mr. De Vis, who has had far 
 better opportunities of studying the question, remarks—‘ Phascolonus, Owen, is 
 demonstrably good; but the ground on which it has been separated—namely, by 
 identification with Sceparnodon, a determination so improbable in itself that nothing 
 short of direct proof should suffice to give it currency—appears to me quite inadequate 
 to say the least.” Not only does Mr. De Vis combat the view that the teeth known as 
 Sceparnodon Ramsayi “ grew in the upper jaw of Phascolonus,” but he believes that 
 * they include the teeth from both jaws of the otherwise unknown animal.’ { His reasons 
 for this opinion are too lengthy for quotation here, but are well worth perusal by those 
 interested in the question. His final paragraph is—‘‘ It must be concluded that both 
 
 
 
 
 
 * Cat. Foss. Mam. Brit. Mus., Pt. 5, 1887, p. 159; and Proc. R. Soc., xlix., p. 60. 
 + Proc. Linn. Soc. N. 8. Wales, 1891, vi. (2), p. 237. 
 t Ibid., p. 258, 
 
682 
 
 the upper and lower incisors of Sceparnodon are known, and, consequently, that 
 Sceparnodon is not a synonym of Phascolonus.” There is much to be said for the bold 
 conception given when defining the Family Nototheride—viz., ‘‘ Probability is also in 
 favour of Sceparnodon proving to belong to this family.’’* 
 
 The geographical range of Sceparnodon is a wide one, as teeth have been found 
 in the vicinity of Lake Eyre, South Australia; and in addition to the Queensland 
 locality a number have been found in the rich bone deposit of Myall Creek, near 
 Bingara, N.S. Wales, by Mr. Charles Cullen, Collector to the Geological Survey 
 of N. 8S. Wales. 
 
 Loc. and Horizon. King’s Creek, Darling Downs (The late C. H. Hartmann— 
 Colin. Australian Mus.; C. W. De Vis—Colln. Queensland Mus.)—Fluviatile deposits. 
 
 Order—SIRENIA. 
 Family—MANATID. 
 
 Genus—CHRONOZOON, De Vis, 1883. 
 (Proc. Linn. Soc. N.S. Wales, viii., Pt. 3, p. 395.) 
 
 CHRONOZOON AUSTRALE, De Vis. 
 Chronozoon australe, De Vis, Loc. cit., p. 395, t. 17. 
 
 Obs. A portion of a skull, consisting of the parietal and upper part of the 
 occipital bones of a non-marsupial animal, has been described by Mr. De Vis, and com- 
 pared to the corresponding portions of a Dugong. 
 
 The chief difference between the fossil and the skull of the Dugong consists in 
 a shallower temporal fossa and feebler muscles for working the jaws. 
 
 A mould taken from the interior surface of these bones has enabled the Author 
 to study the brain characters with much success. 
 
 The brain was clearly of inferior development to those of existing Sirenians, 
 “and a smoothness of skull indicatory of feebler masticating power, may have been 
 the ¢o-adaptation of the softer vegetation and less perilous condition of life enjoyed by 
 a Sirenian tenant of fresh waters.” 
 
 Loc. and Horizon. Chinchilla, Darling Downs (C. W. De Vis—Colln. Queens- 
 land Mus.)—Fluviatile deposits, associated with Crocodile, Turtles, Ceratodus, and the 
 remains of land animals. 
 
 Order—UNGULATA, 
 Family—DICOTYLIDZ. 
 
 Genus—PROCHZRUS, De Vis, 1886. 
 (Proc. R. Soc. Queensland, iii., p. 47.) 
 
 PROCHHRUS CELER, De Vis. 
 Procherus celer, De Vis, Loc, cit., p. 47, t. 1. 
 
 Obs. The occurrence of various peculiar teeth in the Post-Tertiary Beds of 
 Darling Downs has led Mr. C. W. De Vis to suggest the former presence in Australia 
 of a swine-like animal, more nearly allied to the Peccary (Dicotyles) than to the true 
 Pigs. The teeth so determined are a quinque-tuberculate tooth of bunodont type, of 
 the general shape of the last lower molar of Dicotyles torquatus, Cuv.; a middle lower 
 
 
 
 * Proc. Linn. Soc. N. 8. Wales, 1891, vi. (2), p. 164. 
 
683 
 
 incisor of the left side ; several second upper incisors, and a portion of the crown of a 
 compressedly triangular tusk. These are described in detail by Mr. De Vis, and 
 compared with their supposed living homologues. On the general question the Author 
 remarks :—‘ It is truly a remarkable fact that New Guinea swine have never, to our 
 knowledge, accomplished the short passage between the northern and southern shores of 
 Torres Straits, or, having done so, failed to establish themselves where the European pig 
 finds it easy to recover and maintain its independence.’ He concludes by stating that 
 the comparative frequency of its teeth shows that it was not altogether a rare member 
 of the Post-Pliocene Fauna of Queensland. 
 
 Loe. and Horizon. Sharrow and other localities, Darling Downs (0. W. De Vis— 
 Colln. Queensland Mus.)—Fluviatile deposits. 
 
 Order—PROBOSCIDEA. 
 Family—ELEPHANTID2. 
 
 Genus—NOTOELEP HAS, Owen, 1882. 
 (Proc. R. Soc., xxxiii., p. 448.) 
 
 NoToOELEPHAS AUSTRALIS, Owen. 
 Notoelephas australis, Phil. Trans. 1883, clxxiii., Pt. 3, p. 777, t. 51. 
 
 Obs. This genus and species were founded on portions of a tusk indicating a 
 mammal larger than Déprotodon, in fact the largest fossil mammal yet foreshadowed 
 amongst the extinct Australian forms. Sir Richard Owen appears to regard it as a 
 Proboscidian Placental. He says, ‘‘ Supposing the dingo to be a human introduction 
 into the Australian Continent,* we here have a gyrencephalous exception to the 
 characteristic aboriginal mammalian organisation of that remote southern continent.” 
 He does not appear to apprehend any connection between this tusk and the molar tooth 
 formerly described by him, and forming a portion of the late Count P. EH. de Strzelecki’s 
 Collection. Prof. Owen remarks that this molar is too large to be associated with the 
 tusk, supposing the latter to have come from the upper jaw of a full-grown individual 
 of its species. Up to the time of the publication of his “ Fossil Mammals of Australia,” , 
 Owen had received no confirmatory evidence from the Australian Continent of the 
 former existence of any animal to which this molar could have belonged. 
 
 Grave doubts have been expressed by several Writers as to the probability of 
 this tooth as an Australian fossil, and it would perhaps be better to expunge it from the list. 
 
 Loc. and Horizon. Darling Downs (The late F. N. Isaac)—Fluviatile deposits. 
 
 In closing this very brief and imperfect account of the Post-Tertiary vertebrate 
 remains of Queensland, it may not be out of place to refer to the “‘ Great Bone Beds” of 
 Mount Guthrie, Berserker Ranges, near Rockhampton. From the notes of the late Mr. 
 James Smith, who investigated this deposit, it would appear to be a tufaceous limestone 
 containing the remains of leaves and shells, probably Helix, but I have not been able to 
 satisfactorily determine the presence of bones in the specimens I have seen. The 
 matrix very much resembles the Hobart Travertin, but is more friable and stalagmitic, 
 and lighter in colour. 
 
 E. 
 
 * Ample evidence now exists to show that the Dingo was coeval with these extinct marsupials both in 
 New South Wales and Victoria. 
 
CHAPTER XXXVIILI. 
 
 THE GEOLOGY OF BRITISH NEW GUINEA. 
 
 Mr. A. Gibb Maitland, of the Geological Survey of Queensland, travelled exten- 
 sively in New Guinea and the adjacent islands from May to September, 1891, and since 
 his return has made a valuable Report, of which I am enabled, through the kindness of 
 His Honour Sir William Macgregor, to give a brief reswmé. The Report embodies 
 not only Mr. Maitland’s own observations, but also a digest of those of previous 
 observers, and is accompanied by Geological Maps. 
 
 Mr. Maitland gives the following table of Geological Formations :— 
 
 Recent Superficial Deposits— Wide Plains along the Rivers ; Coastal Flats, &e. 
 
 Coral Reefs, Coral Islands, Upraised Reefs, and associated deposits. 
 
 Kevori Grits: Post-Tertiary—Grits, Sandstones, and Conglomerates. 
 
 Port Moresby Beds: Tertiary ?—Greenish Sandy Shales, Limestones, Calcareo- 
 Siliceous Beds of Port Moresby. 
 
 Boioro Limestones, of undetermined age—Greyish Limestones, &c., of Boioro 
 and the Coast. 
 
 Metamorphic Rocks, of undetermined age—Schists, Slates, Gneiss, Kc. 
 
 Igneous Rocks—Basalt and other Volcanic Rocks, Ashes, &c. 
 
 Plutonic and Intrusive Rocks—Diorite and other Basic Plutonic Rocks, 
 Granite, Mica-Trap, &c. 
 
 RECENT SUPERFICIAL DEPOSITS. 
 
 Recent Superficial Deposits are represented as commencing on the Southern 
 Coast at the mouth of the Vanapa River, west of Port Moresby, and occupying a belt 
 _of country which gradually widens until, at the Dutch Boundary, it covers three out 
 of the four degrees of latitude which comprise the Western limit of the British 
 Possessions. 
 
 CORAL REEFS, CORAL ISLANDS, UPRAISED REEFS, AND ASSOCIATED DEPOSITS. 
 
 The exigencies of rapid travel did not permit Mr. Maitland to examine any of 
 the existing coral reefs, but opportunities occurred of observing many of the upraised 
 reef masses, especially at Einauro (Cette) Island, Ware (Teste) Island, the Bell Rock, 
 Pannietta Island, Kimuta (Renard) Island, Misima (St. Aignan) Island, and along the 
 north-east coast. The latter present “all gradations, from reefs only a few feet above 
 the water up to two thousand feet above the level of the sea.” 
 
 Mr. Maitland gives the following description of the upraised reefs :-— 
 
 “The rocks present pretty much the same lithological characters throughout— 
 viz., very hard and sonorous compact limestones, of a whitish colour. Some varieties are 
 of a distinct yellow or reddish-brown colour. Coral fragments do not appear to be very 
 common ; but in some of the upraised reefs molluscan remains are by no means rare. 
 The limestones, in the majority of instances, are seamed with veinlets of carbonate of 
 lime. 
 
 “Generally the structure of the coral has been destroyed by the action of infiltrating 
 water. Instances, however, do occur—e.g., at Misima—in which this is not the case. 
 
685 
 
 Here the base of one of the upraised reef masses consists of a chalky limestone, in which 
 the remains of corals still exist. In most of the islands and localities examined, these 
 elevated reef masses, when viewed at a distance, present the appearance of vertical 
 
 walls and level terraces stretching often for considerable distances. The faces of these 
 ‘cliffs are sometimes covered with vegetation to such an extent as to present the 
 appearance of consisting of a huge wall a foliage. 
 
 “The reefs raised only a few feet above the sea level, such as those of Pan- 
 nietta, present, along the shore, a white perpendicular cliff, of varying height, above 
 which is an almost level tableland, very broken and rugged, and with a very uneven 
 surface. 
 
 “Gigantic ‘ swallow-holes’ and enormous caves have been carved out of some of 
 the limestones, and are lined with stalagmites and stalactites. The faces of the limestone 
 cliffs are weathered into most rugged and sharp-edged forms, often presenting features 
 of great beauty. 
 
 “In the majority of cases which came under my notice, the various limestone 
 terraces were horizontal, but at Ware (Teste) Island a marked peculiarity of the reef 
 limestones was their disposal into a series of gentle folds, the axes of which trended, 
 roughly, north and south. In Einauro (Cette) Island, the cream- -coloured limestone 
 had a dip of 50 degrees to the west-north-west.” 
 
 As the collection of fossils from the upraised reefs has not yet been critically 
 examined, no definite information can be given regarding the age of the deposits. I 
 may remark, however, that there is nothing in the evidence accumulated by Mr. 
 Maitland to warrant an inference which might be hastily drawn from the position 
 occupied by the upraised reefs on his scale of classification—viz., that the elevation— 
 extending to at least two thousand feet—attested by the altitudes attained by the reefs, 
 took place entirely since Tertiary times. The process of elevation may have been going 
 on continuously from a period much further back in the geological story. Indeed the 
 comparatively unimportant altitudes attained by Tertiary rocks may be taken as evidence 
 (however incomplete, and to some extent merely of negative value) that the position 
 of these latter rocks forms a measure of the elevation accomplished since Tertiary 
 times. 
 
 KEVORI GRITS: POST-TERTIARY. 
 
 Under this name Mr. Maitland describes a Series of Sandstones, Grits, and 
 Conglomerates, which, in the Kevori District, north-west of Hall Sound, rest directly 
 upon the Port Moresby Beds. The strata in question have been little disturbed from their 
 original horizontal position, but in places they dip at a low angle to the north-east. 
 Mr. Maitland observes :—‘‘ That the Kevori Grits are younger than those which have 
 been called the Port Moresby Beds, and which are regarded by Mr. R. Etheridge, Junr., 
 as being Miocene* or Pliocene Tertiary, is all that the meagre evidence at present 
 collected permits us to say.” 
 
 PORT MORESBY BEDS: TERTIARY. 
 
 These beds occupy a considerable area of country, fringing the coast from 
 Caution Bay south-eastward to McFarlane Harbour, and extending inland for about 
 twenty miles up the Kemp-Welch River. They consist of sandy limestones and fine- 
 grained calcareous shales, with black and yellow lenticular nodules of flint and 
 chalcedony, and are generally vertical, or inclined at high angles. 
 
 * A Miocene age was ascribed to these fossils by the late Mr. C. 8. Wilkinson, not by me. I am in 
 acgord with the late Rev. J. E. T. Woods, as explained later on, that these fossils are much more likely to 
 be of Pliocene age, and probably even to one of the younger divisions of that Formation, (2,2, Junr.) 
 
686 
 
 From these beds Mr. Maitland obtained a suite of fossils, which, however, have 
 not yet been critically examined, but he provisionally names the following :— 
 
 GASTEROPODA. 
 Conus. 
 Turritella. 
 LAMELLIBRANCHIATA. 
 Cardita. 
 Pecten nove-guinee, Ten. Woods ? 
 Pectunculus. 
 Venus. 
 And fragments of undeterminable corals. 
 
 CRETACEOUS. 
 
 Mr. Maitland does not locate on his Geological Maps, nor does he find a place in 
 his table of formations for the strata containing the Cretaceous fossils referred to by 
 the late Mr. C. 8S. Wilkinson and my Colleague,* although he quotes from the writings of 
 both these gentlemen on the subject. The fossils in question, together with a further 
 collection forwarded by the Administrator in the beginning of 1890,+ are enclosed in 
 water-worn boulders and pebbles of white limestone occurring above the confluence of 
 the Strickland with the Fly River. They do not appear to have been found iz situ. The 
 last-mentioned collection consists mainly of corals. As my Colleague comments fully 
 on the Fly River fossils, it is unnecessary for me to say more. 
 
 BOIORO LIMESTONES (AGE UNDETERMINED). 
 
 “ What have been called the Boioro Limestones are best exposed in that headland 
 in Launoka Division (Mayri Bay) from which the beds are named. 
 
 ‘At Boioro, the limestones are of a leaden-grey colour, and are seamed with 
 veinlets of carbonate of lime. The weathered surfaces present a curious brecciated 
 aspect. The bedding-planes, marked by lines of brecciated fragments (?), are inclined to 
 the north-west, at angles varying from 35° to 40°. Some of the limestones contain 
 flint nodules ; in some places there is a gradual passage from limestone into flint. A 
 dyke of dolerite was seen to penetrate the limestones in the cliffs of Boioro. 
 
 ‘“‘On the very feeble evidence of lithological similarity, the limestones of Rogea 
 (Heath) Island, and the Mainland north of Samarai, in the vicinity of Waiera Creek, 
 are denoted by the same colour as those of Boioro. The Rogea Limestones are arranged 
 in thin beds in a small synclinal trough. The limestones of the Mainland are identical 
 in every way with those of Rogea. In neither place did they yield any organic remains. 
 
 “The limestones of the Mainland are penetrated by dykes of dolerite, and 
 sections show what have every appearance of being interbedded dolerite sheets. 
 
 “There is no evidence as to the age of the beds. From their position they 
 appear, prima facie, to be beneath the Port Moresby Beds, and they present totally 
 different lithological characters to those possessed by the latter. They are uncon- 
 formably overlaid by the Recent Volcanic Rocks.” 
 
 Referring, in a foot-note, to the Boioro Limestones of Mayri Bay and Port Glasgow, 
 Mr. Maitland suggests that the limestones ‘“‘may be merely portions of an upraised 
 coral reef,’’ and observes that “ the adjacent island of Cette is obviously of this nature.” 
 
 
 
 * The only fossil referred to by me as perhaps of Cretaceous age is an Inoceramus or Aucella, the great 
 bulk of the secondary fossils (Ammonites) being regarded as of uppermost Oolite age. (R.Z. Junr.) 
 
 + Letter dated 6th May, 1890, from the Writer to the Administrator of the Guvernment of British 
 New Guinea. Appx, Z. to the Administrator's Annual Report for 1890-91. Brisbane: by Authority: 1892. 
 
687 
 
 From what has already been said regarding the age of the upheaval of the coral reefs, 
 it will be seen that there is not necessarily anything in Mr. Maitland’s suggestion 
 inconsistent with the assignment of an early Tertiary, or Pre-Tertiary, date to the 
 Boioro Limestones. . 
 
 From observations made by Mr. Maitland at Millport Harbour, it is evident that 
 the Boioro Limestones have a thickness of at least 800 feet. 
 
 METAMORPHIC ROCKS. 
 
 The approximate definition of the area occupied by these rocks, in which, and the 
 granitic and other plutonic rocks, deposits of the “precious” and less precious metals 
 may be looked for, is, from an economic point of view, one of the most important 
 results of Mr. Maitland’s observations. 
 
 The Metamorphic Rocks are separable, according to Mr. Maitland, into two broad 
 subdivisions. ‘The first includes what may be called the crystalline schists, and the 
 second comprises all those other rocks in which the alteration has not gone sufficiently 
 far to conceal their clastic or derivative nature. To draw a line separating the two 
 divisions is quite impossible at present.” 
 
 An immense area, extending for a few miles back from Port Moresby, nearly to 
 the 8th parallel of South Latitude (the German Boundary) is occupied by Metamorphic 
 rocks, Another large area occurs on the Mainland to the east, at Mount Suckling. 
 Although unexplored, the greater part of the intervening district, and indeed probably 
 the greater part of the highland interior of New Guinea, may be conjectured to be of 
 similar constitution. The islands of the D’Entrecasteaux and Louisiade Groups, 
 several of which are known to be auriferous, are also mainly composed of metamorphic 
 rocks. It will remain for future geologists to determine whether, among these rocks, 
 the representatives of our “‘Gympie” and “ Burdekin’? Formations, and of the still 
 older formations not yet recognised in Queensland, are to be distinguished. 
 
 IGNEOUS ROCKS. 
 
 From Mr. Maitland’s Maps it appears that volcanic rocks are met with at intervals 
 from the Douglas River (Long. 144° 15’ E.) to the Eastern end of New Guinea and 
 throughout the D’Entrecasteaux Islands, where they occupy considerable areas. In the 
 Louisiade Archipelago they seem to occur more sparingly, or, at least, they have not 
 been noted east of Long. 152° 40’, where they form some of the smaller islands of the 
 group. Mr. Maitland says that “the Volcanic rocks fall into two primary divisions, 
 the Acidic Series and the Basic Series, the former of which appears to predominate. 
 Representatives of the Trachytic, Andesitic, and Basaltic lavas, with their associated 
 fragmental beds, were met with throughout the Possession. From the fact that these 
 rocks rest, with a violent unconformability, on the most recent strata, they cannot be of 
 any very great age.” 
 
 Interesting particulars are recorded of some forms of modified volcanic activity 
 in the D’Entrecasteaux Islands and the Mainland of New Guinea. 
 
 In Fergusson Island, the largest of the D’Entrecasteaux Group, Captain 
 Moresby, Mr. Andrew Goldie, Mr. Basil H. Thompson, and Sir William Macgregor 
 have noted the occurrence of thermal springs. Sir William records that “ the whole of 
 the low country near Seymour Bay contains, here and there, over an area of, perhaps, 
 eight or ten square miles, boiling springs, saline lakes, and thousands of fumaroles, 
 giving out sulphur fumes.” Mr. Thompson describes “springs of boiling water and 
 boiling mud,” and adds that “in one instance boiling mud was spouted up from a 
 
 chimney-like cavity in the hillside.’ 
 
688 
 
 In Fergusson Island (Moratau)* Mr. Maitland ascended the Crater of Diau, 900 
 feet. ‘‘ The ascent was made up a gully carved out of a blackish ash, with fragments of 
 pumice-stone and a glassy volcanic rock. From the summit an excellent view of the 
 cone and its associations could be obtained. This is a tuff cone. Its south-eastern face 
 is hollowed out into numerous ravines, in which occasional sections show stratified ashes. 
 The crater wall has been breached by a lava, which flowed to within a short distance of 
 the beach, near Worua Island. 1 followed the edge of the lava-flow from its source to its 
 termination, and was enabled to ascertain that its general character is similar throughout. 
 The rock has a glassy resinous lustre and a splintery fracture. Weathered surfaces show 
 undoubted fluxion-structure, the lines of flow sweeping round the sanidine crystals, 
 sanidine being the only mineral visible to the eye. From the summit of the crater the 
 emanation of water-vapour could be seen over a large area of country to the north.” 
 
 In referring to the small bay in Fergusson Island, to the north-west of Rawat 
 Point, Mr. Maitland observes that “ its peculiar scythe-shaped form pointed to its being 
 the segment of an ancient crater, and an actual examination gave credence to this view. 
 Manifestations of solfataric action were evident on the face of the cliff. . 
 Tn places the sea water was quite hot, owing to the streams of hot water which flowed 
 down from the hills behind.” 
 
 Mr. Maitland describes two visits made by him to the island of Dobu (Goulvain), 
 south of Fergusson Island, ag follows :— 
 
 ‘Approaching Dobu from Dawson Straits, it appeared to have all the 
 characteristics of a voleano. Steam could be seen issuing from points on the beach on 
 the north side of the island. 
 
 “My first visit was paid at about the time of high water. There were several 
 orifices from which water issued at an average temperature of 200° Fahr. I estimated 
 the area over which the waters issued at about one hundred square yards. The gas, 
 given out copiously, had a strong sulphurous odour. The sandstones in the neighbour- 
 hood were slightly bleached, | 
 
 “A second visit, at low water, showed that the so-called boiling springs were 
 merely fissures to which sea water had access. The sides of the fissures were encrusted with 
 deposits of flowers of sulphur. A few yards behind the fumaroles was a whitish-grey cliff, 
 exhibiting undoubted evidences of solfatarie action. In caverns in the cliffs there occur 
 large deposits of yellow and greyish-brown sulphur, commonly massive, but here and there 
 in the form of acicular crystals. These caverns, many of which I discovered when 
 breaking down the cliffs with my hammer, were found to have a very high temperature. In 
 one case a stream of hot air rushed out witha hissing noise, but this was only momentary.” 
 
 In the same island there are two extinct craters, which must be of considerable 
 proportions, for Mr. Maitland mentions that ‘“‘a few villages” have been built on the “lofty 
 almost circular wall, roughly estimated at about a hundred feet in height,” of one of them. 
 
 Mr. Maitland got sufficiently near the active voleano of Mount Victory (on the 
 north-east coast of New Guinea), to see volumes of steam and smoke issuing from the ° 
 sides of the mountain. 
 
 PLUTONIC AND INTRUSIVE ROCKS. 
 
 The area occupied. by granitic rocks is apparently not large. So far as 
 exploration has extended, it has only been noted in the Mainland at Mabadaan, north 
 of Sabai Island, and in a few of the islets of Torres Strait. Diorites and other basic 
 rocks, which Mr. Maitland regards as either Plutonic or Intrusive, are met with in 
 limited areas in the Owen Stanley District. 
 
 a ea ee a ee 
 
 * In the 1890 Map the name Moratau is applied to Goodenough Island, west of Fergusson Island, 
 
689 
 
 ECONOMIC GEOLOGY 
 
 Gold.—Alluvial gold has been worked in the Islands of Saint Aignan and 
 Sudest, and is known to exist also in Normanby Island, in the Vanapa River, and in the 
 Saint Joseph District. In Normanby Island the gold is associated with cinnabar. Reefs 
 are worked on a small scale in Sudest Island, and have been noted in Normanby 
 Island. In the years 1888 to 1891, inclusive, 8,399 oz. of gold, valued at £34,310, have 
 been reported to the Customs at Cooktown, from New Guinea.* 
 
 Sulphur.—Native sulphur occurs in Fergusson and Goulvain Islands, in the 
 D’Entrecasteaux Group. 
 
 Lignite.—Seams of lignite are known in Yaru Island, and on the Fly and 
 Strickland Rivers. 
 
 Mercury,—Cinnabar has been found in small quantities at Merani, in Cloudy 
 Bay, and in Normanby Island. 
 
 J. 
 
 
 
 * ««That gold exists in the western and northern portions of New Guinea has long been known; that 
 it exists also on the south-eastern shores of that great island is equally true, as a specimen of pottery 
 procured at Redscar Bay contained a few laminar grains of this precious metal. The clay in which the gold 
 is imbedded was probably part of the great alluvial deposit on the banks of the rivers, the mouths of which 
 we saw in that neighbourhood, doubtless originating in the high mountains behind, part of the Owen 
 Stanley Range.”—MacGillivray. Narr. Voyage of H.M.S. “Rattlesnake,” &c., 1852, ii., p. 69, 
 
 2V 
 
CHAPTER XXXIX. 
 
 PALZONTOLOGY OF BRITISH NEW GUINEA. 
 
 As might naturally be expected, but little is known of the Paleontology of New 
 Guinea. The existence of fossiliferous Tertiary rocks was announced in 1876, by the late 
 Mr. C. 8. Wilkinson, who based his determination on a small collection made by the late 
 Sir William Macleay, at Yule Island, during the ‘‘ Chevert” Expedition. Post-Tertiary 
 deposits were shown to exist by the late M. de Miklouho-Maclay, on the Maclay coast; 
 and since then shells of the same age have been met with at the Aird Hills, Douglas 
 River, by Mr. Theodore Bevan. 
 
 Rocks of Mesozoic age exist in New Guinea, as evidenced by Ammonites brought 
 from the Strickland River by the late Expedition of the Australian Geographical 
 Society. Although these are only rolled specimens from the river-bed, they 
 satisfactorily show the presence there of deposits of Oolite age, probably about the 
 horizon of the uppermost Oolites. Lastly,* my Colleague’s Collection contains a few 
 Tertiary Corals and Mollusca from Maiva, collected by Mr. E. Edelfelt. 
 
 DESCRIPTION OF THE SPECIES. 
 Kingdom—ANIMALIA, 
 Sub-Kingdom—C@iLENTERATA. 
 
 Class—ACTINOZOA. 
 
 The Collection of the Queensland Geological Survey has been enriched by 
 the presentation of some hand specimens of a brownish-yellow marl, by Mr. E. 
 Edelfelt, from New Guinea. This marl has plentifully scattered through it the 
 remains of small shells in the form of casts anda few fragments of corals. The locality 
 is Maiva Village, at a height of about two hundred feet above the sea-level. Although 
 these fossils are very fragmentary, “any Tertiary Marine remains from the Pacific are of 
 high interest, because of their bearing on the coral reef theory.” + 
 
 The most striking of the corals is a species of Alveopora, allied to those described 
 by Dr. A. E. Reuss from the Tertiary Beds of the Tiji-Lanang Valley, Rongga District, 
 Java.~ The trabecular septa are strong and spine-like, much curved, and six or 
 perhaps more ina cycle. They have this peculiarity, that they appear to be developed. 
 in pairs—a character to some extent seen in Reuss’ specimens, but in the present fossils 
 carried to a much higher degree. The spurious columella formed by the union of the 
 septa is of the slightest construction. Jn the character of the septa this coral appears 
 
 
 
 *Sir William MacGregor, Administrator of British New Guinea, has forwarded a collection of rolled 
 coral specimens from the Fly River, evidently brought down the course of that stream from its upper 
 sources, where, doubtless, the rocks from which these are derived are in place. Many of the corals present 
 excellent material for microscopic examination, but the absence of the necessary works of reference for their 
 elaboration has so far prevented the Writer from progressing with the work. 
 
 + Tenison Woods, Proc. Linn. Soc. N. S. Wales, 1879, iv., p. 539. 
 
 { Ueber fossile Korallen yon des Insel Java. Reise Osterr. Fregatte Novara, 1857-59. Geol. Thiel, 
 ui, Band, 2 Abth., p. 165, 
 
: 691 
 
 to be most nearly allied to Alveopora brevispina, Reuss,* but in the other features to 
 A. hystrix, Reuss.¢ If the paired condition of the septa, here so very marked, is a 
 constant and definite character, and it appears to be so, it will at once distinguish this 
 coral from all those described by Dr. Reuss. 
 
 : The largest and best-preserved coral is a species of Leptoria, a genus not met 
 with either by Reuss amongst the Javan corals, nor by Prof. K. Von Fritsch,t amongst 
 those collected in Borneo by Mr. R. D. M. Verbeek. On the other hand, Prof. K. 
 Martin, of Leiden, describes § an allied genus, Celoria, from the former country. The 
 characters of the New Guinea Leptoria, as pourtrayed in the single specimen, are not 
 sufficiently clear for specific description, and make one long for further material. 
 Leptoria is extensively distributed in the Indian and Pacific Oceans. 
 
 Next in order is a well-marked Galaxea, again only a fragment, but clearly not 
 far removed from the recent G. clavis. The corallum, as preserved, is split in half 
 longitudinally, and exhibits several corallites radiating outwards and surrounded by a 
 copious peritheca. 
 
 The last to be noted, but certainly not the least important, are two examples, 
 fragmentary unfortunately, of the interesting genus Deltocyathus, distinet both 
 from the Tertiary and Recent species D. italicus, Ed. and H., and the recent D. 
 magnificus, Mosely. The occurrence of this genus in these New Guinea beds is of the 
 highest interest, following as it does upon its discovery by the “ Challenger’’ Expedition 
 in the Pacific. || 
 
 The material presented by Mr. Edelfelt to the Queensland Survey Collection is 
 of too limited a nature to permit any definite statement to be made as to the age of the 
 beds, but they are either Younger Miocene or Pliocene, probably the latter. The Javan 
 series described by both Reuss and Professor Martin are considered by the latter to be 
 of Miocene age. 
 
 Sub-king¢dom—ECHINODERMATA. 
 Class—ECHINOIDEA. 
 
 Order—ENDOCYCLICA. 
 Family—TEMNOPLEURIDA. 
 
 Genus—TEMNECHINUS, Forbes, 1852. 
 Mon. Brit. Tertiary Echini, p. 5.) 
 
 TEMNECHINUS Macteayana, Zen. Woods. 
 Temnechinus Macleayana, Ten. Woods, Proc. Linn. Soc. N.S. Wales, 1877, ii., Pt. 2, p. 126. 
 
 Sp. Char. Test small, depressed, circular, and the ambitus rounded; actinal 
 surface slightly rounded and depressed to the actinostome; interambulacral areas 
 twice the width of the ambulacral at the ambitus, and about one-third broader at the 
 mouth, slightly depressed in the middle by an undulating line of suture, which 
 
 * Loc. cit, t. 3, 1. 1 a-c. 
 
 + Ibid., t. 3, f. 8a-c. 
 
 + Fossile Korallen der Nummulitenschichten von Borneo. Palacontographica, Suppl. 1878. Band. iii. 
 Lief, 1, Heft. 3, p. 93.) 
 
 § Die Tertiirschichten auf Java, 2 Thiel., p. 137 (folio, Leyden, 1880). 
 
 || Report on certain Hydroid, Aleyonarian, and Madreporarian Corals, &c., by Prof. Mosely. Voy 
 Challenger, vol. ii., Zoology, 1881, pp. 147 and 148, 
 
 { Loc, cit., 2 Thiel, p. 38, 
 
692 
 
 becomes a very distinct depression on the abactinal surface, on which the line of the 
 plates are well marked; pores in a vertical row, slightly oblique, and their zones sunken. 
 Interambulacra have two rows of primary tubercles, each row being flanked again on 
 each side by a vertical row of secondaries, all small and imperforate, both primaries and 
 Secondaries surrounded by circles of granular tubercles, which are frequently con- 
 nected with the main tubercle by a ridge. Primaries of the ambulacra in two vertical 
 rows, each close to its poriferous zone; secondaries not so visible, but the rings of 
 granules are very manifest, with an indented vertical line of suture in the centre. 
 Actinal opening larger, with conspicuous but not deep indentations. Diameter, sixteen ; 
 altitude, six millim. (Zen. Woods.) . 
 
 Obs. Mr. Woods appears to consider this near the Zemnechinus lineatus, 
 Duncan,* from the Mordialloe beds, Hobson’s Bay, but, again, he adds—“ The nearest 
 affinities are Z. globosus, of the British Crag.” The species is provisionally named only. 
 
 Loc. and Horizon. Yule Island, New Guinea (The late Sir W. Macleay— 
 Macleay Museum, University of Sydney) —Lower Pliocene ? 
 
 Family—LAGANIDZ. 
 
 Genus—PERONELLA, Gray, 1855. 
 (Cat. Recent Echini Brit. Mus., Pt. 1, 1855, p. 13.) 
 
 PERONELLA DECAGONALIS, Lesson, sp. 
 
 Peronella decagonalis (Lesson), Agassiz, Revision (Echini Il. Cat. Mus. Comp. Zool. Harvard Coll., 1872, 
 No. vii., Pts. 1 and 2, p. 148. 
 1 7 Ten. Woods, Proc. Linn. Soc. N. 8S. Wales, 1877, ii., Pt. 2, p. 126. 
 
 Obs. This has been recognised by the late Rev. J. E. Tenison Woods asa 
 fossil from Yule Island, New Guinea. He says—‘“ The specimens, two in number, are 
 extremely thin and concave,on the actinial side, but they are both young specimens, and 
 one scarcely above an inch in diameter.’ 
 
 Loc and Horizon. Yule Island, New Guinea (The late Sir W. Macleay— 
 Macleay Museum, University of Sydney)—Lower Pliocene ? 
 
 
 
 Sub-Kingdom—MOLLUSCA. 
 
 Class—PELECYPODA. 
 
 Order—OSTRACEA. 
 Family—PECTINID. 
 Genus—PECTEN, O. F. Miller, 1776. 
 
 (Zool. Danice Prod., p. xxxi.) 
 
 PECTEN NoVH-GUINER, Ten. Woods. 
 Pecten nove-guinew, Ten. Woods, Proc. Linn. Soc. N, 8. Wales, 1877, ii., Pt. 3, p. 267. 
 
 Sp. Char. Shell regularly orbicular, equivalve, regularly convex, but not: 
 globose, equilateral, and symmetrically rounded at the margin; ears quite square, one 
 being a little obliquely indeuted at the edge, but otherwise almost equal, and rather 
 large, and with from eight to ten very granular ribs; surface with from twelve to 
 
 
 
 * Quart, Journ. Geol, Soc., 1877, xxxili., pp. 46 and 65, t. 3, f, 3-5, 
 
693 
 
 fourteen large rounded radiate ribs; each with two rather shallow radiate grooves and 
 transversely striate, strie at the marginal end becoming scaly raised imbrications, eight 
 to ten in number ; interstices furnished with two or three conspicuous granular ribs ; 
 umbone very acute ; Long. 60, Lat. 50, thickness of two valves 30 millim. (Zen. Woods.) 
 
 Obs. This shell is said by its describer to have relations with Pecten asper, of 
 South Australia, the common Australian P. bifrons, and P. radula, Linn., from the 
 Philippine Islands, but to be distinct from all. 
 
 Loc. and Horizon. Yule Island (The late Sir W. Macleay—Macleay Museum, 
 University of Sydney)—Lower Pliocene ? 
 
 Order—VENERACEA. 
 Family—CYRENIDZ. 
 
 
 
 Genus—-CYRENA, Lamarck, 1806. 
 (Ann. Mus. Hist. Nat. Paris, vii.) 
 
 Crrena nitipa, Deshayes. 
 
 Cyrena nitida, Deshayes, Proc. Zool. Soc., 1854, p. 28. 
 x a Canefri, Ann. Mus, Civ. Storia Nat. Genova, 1883, xix., p. 286. 
 
 Obs. This species is reported from the Aru Islands, by Canefri; and he quotes 
 New Guinea, on the authority of Beccari. 
 
 Loc. and Horizon. Aird Hills, Douglas River, British New Guinea. This 
 species, with Melania clavus, Lamarck, and Neritina gagates, Lamarck, was collected by 
 Mr. T. F. Bevan during his Fifth Exploring Expedition to British New Guinea. He 
 says—‘‘The term Aird Hills describes an island of probably moderately recent 
 upheaval, on which a cluster of volcanic cones, some ten in number, and covering an 
 area of about five square miles, are surrounded by deep navigable channels of fresh 
 water. The country for thirty miles to the south, and for some ten miles to the north, 
 is chiefly of low-lying alluvial formation. The general form of these trachyte hills is a 
 volcanic cone. The summit of this particular cone, however, is covered with a deposit 
 of semi-fossilised fluviatile shells, contained in an earthy mould or silty mud.’”’* 
 
 Class—GASTEROPODA. 
 
 Order—PECTINIBRANCHIATA. 
 Family—MELANIDZ. 
 
 Genus—MELANIA, Lamarck, 1801. 
 (Syst. Anim. sans Vertéb., p. 91.) 
 
 MeELAnrIA ciavus, Lamarck. 
 
 Melania clavus, Lamarck, Loc. cit., 1822, vi., Pt. 2, p. 165. 
 A AS Brot, in Kuster’s Syst. Conch.—Cabinet, 1874, Melaniaceen, p. 175, t. 21, f. 17 a-c. 
 
 Obs. Mr. J. Brazier informs me that this species has been met with in the 
 
 Solomon Islands, but not before in New Guinea. 
 Loc. and Horizon. With the preceding. 
 
 
 
 * Mr. T. F. Bevan’s Fifth Expedition to British New Guinea, 1888, pp. 21-22 (8vo.: Sydney : 
 by Authority : 1888). 
 
694 
 
 Family—DOLIID. 
 
 Genus—DOLIUM, Lamarck, 1801. 
 Syst. Anim. sans Vertéb., p. 79). 
 
 Doxrium costatum, Deshayes. 
 
 Doliwm costatum, Deshayes, in Lamarck Hist. Nat. Anim. sans Vertéb., Ed. 2, 1844, ix., p. 144. 
 Fe - Ten. Woods, Proc. Linn. Soc. N. S. Wales, 1878, ii., Pt. 3, p. 268. 
 
 Obs. Characteristic casts of this species have been recorded by the late Rev. 
 J. E. Tenison Woods from the New Guinea Tertiary strata. He remarks—“ There is no 
 other species known to me which has the peculiar sub-acute distant ribs, and decidedly 
 eanaliculate suture, all of which, as well as the corresponding shape, are well shown in 
 the cast in Mr. Macleay’s Museum.” 
 
 These casts are accompanied by others of a Phos, and Strombus nove-zealandia. 
 
 Loc, and Horizon. Yule Island, New Guinea (The late Sir W. Macleay— 
 Macleay Museum, University of Sydney)—Lower Pliocene ? 
 
 Family—NERITID &. 
 
 Genus—NERITINA, Fleming, 1828. 
 (Brit. Animals, p. 321.) 
 
 Neririna GAGATES, Lamarck. 
 
 Neritina gagates, Lamk., Hist. Anim, sans Vertéb., 1822, vi., Pt. 2, p. 185. 
 Reeve, Conch. Icon. (Mon. Weritina), 1855, t. 10, f. 47. 
 Brazier, Proc. Linn, Soc. N. S. Wales, 18 ii., p. 21. 
 oy a Canefri, Ann. Mus. Civ. Storia Nat. Genova, 1883, xix., p. 66. 
 Obs. This species was obtained in the living state by Mr. J. Brazier at the 
 Katau River, in the “ Chevert’’ Expedition. 
 Loc. and Horizon. Aird Hills, Douglas River (2. F Bevan—Mining and Geol. 
 
 Museum, Sydney)—Post-Tertiary. 
 
 ” 9 
 
 9 ” 
 
 A very interesting Paper on the Geology of New Guinea was a few years ago 
 contributed by the late Mr. C. 8S. Wilkinson, Government Geologist of N. S. Wales, 
 “* Notes on a Collection of Geological Specimens collected by William Macleay, Esqr., 
 &c., from the Coasts of New Guinea, &c.”* Amongst these were— 
 
 1. Oolitic limestone from Bramble Bay. 
 2. Yellow calcareous clay from the Katau River. 
 3. Yellow and blue calcareous clays from Yule Island and Hall’s Sound. 
 
 The included fossils led Mr. Wilkinson to regard these clays as of Lower Miocene 
 age, and “exactly similar in lithological character to the Lower Miocene beds near 
 Geelong, and on the Cape Otway coast in Victoria.” 
 
 The larger number of fossils were obtained at Hall’s Sound, and in the condition 
 of casts, but the only two specifically determined were— 
 
 Voluta macroperta, McCoy 
 anticingulata, McCoy. 
 
 ” 
 The evidence for assigning a Miocene age to these beds seems to be anything but 
 conclusive. The deposit at Yule Island is a caleareous concrete, composed of Shells, 
 
 * Proc. Linn. Soc. N.S. Wales, 1877, i., Pt. 2, p. 118. 
 
695 
 
 Corals, and Echini. These are probably the species referred to in previous pages from 
 Yule Island, and described by the Rev. J. E. Tenison Woods in two papers, “On a 
 Tertiary Formation at New Guinea” * and “On some ‘Tertiary Fossils from New 
 Guinea.’’+ He considers these deposits not as old as the Murray River Tertiaries, or 
 those of Cape Otway in Victoria, or Mount Gambier in South Australia. Although 
 this is clearly a criticism of the previously published view of Mr. ©. 8S. Wilkinson, that 
 the New Guinea fossils are referable to the Lower Miocene, no mention whatever is 
 made of that gentleman’s paper on the subject. 
 
 In addition to the shells first described, the late M. de Miklouho-Maclay collected 
 no less than thirty-eight species of Mollusca from a greenish sandy clay forming the 
 nearest hills to the coast line, at the Village of Bongu, Maclay coast.t 
 
 The specimens were determined by Mr. John Brazier, who states § that they all 
 belong to species at present living in the China Sea, in Torres Strait, and around the 
 Philippine Islands. The following is a list of his determinations :— 
 
 Ranella albivaricosa, Reeve Cultellus, sp. ? 
 
 Nassa liquijarensis, A. Adams Corbula crassa, Hinds 
 
 Nassa, sp.? Corbula albuginosa, Hinds 
 
 Mitra, sp.? Mactra, sp.? 
 
 Oliva neostina, Duclos Tellina (Tellinella) Mc Andrewi, Sowerby 
 Oliva sidelia, Duclos Tellina (Arcopagia) pinguis, Hanley 
 Oliva, sp. ? Tellina (Phylloda) foliacea, Linn. 
 Oliva lepida, Duclos Tellina (Angulus), sp. ? 
 
 Oliva ispidula, Sowerby Tellina (Tellinides), sp. ? 
 
 Oliva, sp. Tellina (Peronea) scalpellum, Hanley 
 Oliva, sp. Tellina (Strigella), sp. ? 
 
 Terebra straminea, Gray Tellina (Metis) spectabilis, Hanley 
 Conus (Dendroconus) glacus, Linn. Venus (Chione) calophylla, Phillipi 
 Strombus canarium, Linn, Venus (Chione) imbricata, Sowerby 
 Bulla ampulla, Linn. Dione bullata, Sowerby, sp. 
 
 Atys cylindrica, A. Adams Dosinia canaliculata, Sowerby, sp. 
 Atys cylindrica, var. elongata, A. Adams Leda pullata, Sowerby 
 
 Atys, sp.? Area, sp. ? 
 
 Dentalium longirostrum, Reeve 
 
 
 
 In the “Records of the Geological Survey of New South Wales ” || I contributed 
 a paper “On our Present Knowledge of the Paleontology of New Guinea,” from which 
 the following extract { is taken, bringing the history of the subject up to date :— 
 
 During the comparatively recent Expedition to New Guinea in 1885, fitted out 
 by the Royal Geographical Society of Australasia,** a few fossils were obtained which 
 next claim our attention. From the head of the Strickland River an olive-green mud- 
 stone was obtained, full of comminuted marine fossils, chiefly mollusca. The 
 lithological character of the matrix points to volcanic origin. None of the species 
 were nameable. 
 
 From the first foot-hills of the Upper Strickland River a block of fine 
 sandstone containing Pecten was obtained. This, Mr. A. J. Vogan, who was attached 
 
 
 
 * Proc. Linn. Soc. N. S. Wales, 1878, ii., p. 125. 
 
 + Ibid., p. 267. 
 
 if fbed., 1885, ix., Pb. 4; p. 963. 
 
 § Ibid., p. 988. 
 
 || Vol. i., Pt. 3, 1889, pp. 172-179, Pl. 29. 
 
 Wee 74 
 ** Special Record of the Arrangements of the Exploration of New Guinea. Proc, Geogr. Soc 
 
 Australasia, Special Vol., 1885, p. 157. . 
 
696 
 
 to the Expedition, informed me was in situ. Theshells are too much worn by weather- 
 ing to attempt a specific determination, but they seem to have more of a Tertiary than 
 a Secondary aspect. 
 
 At Observatory Bend, Strickland River, numerous travelled nodules and small 
 boulders were collected, revealing a totally different kind of life, chiefly the remains of 
 Ammonites. But amongst them is a bivalve, either an Awcella or an Inoceramus. If 
 the latter, it is decidedly of the type of the Cretaceous I. concentricus. Unfortunately, 
 the characters of the hinge cannot be ascertained. These fossils are, however, of little 
 importance when compared with the Ammonites. Out of a number of nodules, in 
 which the fossils are indicated by impressions or casts, a fairly representative series has 
 been selected, containing four more or less recognisable species, or at any rate species 
 which can be referred to one or other of the sections into which the old genus 
 Ammonites is now broken up, and the facies of which is sufficiently clear for broad 
 generalisation. 
 
 The section Stephanoceras is largely represented by an Ammonite of the group 
 of A. calloviensis, Sby., and even closely allied to that species. At first sight 
 the primary cost springing from the umbilical margin are not very apparent in 
 our specimens, but attentive examination reveals them as in D’Orbigny’s figure * of 
 this species, but closer together, and therefore more numerous. It would appear that 
 the umbilicus is smaller than in the European form, and less telescopic, wherein these 
 shells approach Stephanoceras transiens, Waagen,t from Kutch, or S. maya, J. de 
 C. Sby.t They possess the same form and arrangement of ribs as in the latter, which 
 commence quite simple at the umbilicus, and break up at about equal distances into 
 bundles of three, whilst the shell is rather more compressed. 
 
 The next species partakes of the form of Stephanoceras Blagdeni, J. Sby., 
 or equally well with S. coronatus, Brug. It is a small shell, with the coste of 
 the back and the tubercles less marked than in the above species. On the other 
 hand, the cross-section of the whorls clearly indicates its relation to this group. 
 The specimen also partakes,in some degree, of the features of the shell figured by 
 D’Orbigny as Ammonites Humphresianus ; § but the umbilicus in the former is deeper. 
 A comparison may also be made with Quenstedt’s figure of S. coronatus ||. 
 
 Two rather well-marked Ammonites appertain to the group Stephanoceras 
 lamellosum, J. de CO. Sowerby,{] but, as compared with that species, possess a 
 wider and more open umbilicus, with the coste of the back less upwardly curved 
 and more horizontal; in fact, the costs are all more direct, and lack the sigmoidal 
 curve on the flanks of S. Jamellosus. From S. Grantianum, Oppel, as figured by 
 Waagen, the cost seem to be finer, but to J. de C. Sowerby’s figure of this species, 
 under the name of 4. Herveyi,** our fossils bear a close resemblance, and also to 
 D’Orbigny’s figuret++ of the same, in the breadth and nature of the back. An affinity is 
 also to be detected in the same Author’s Ammonites macrocephalus,tt but not with that 
 of Waagen under the same name. A third fragment, however, possesses costs as coarse 
 as those shown in the latter’s illustration of Stephanoceras Grantianum. 
 
 * Pal. Franc. Terr. Jur. Ceph., i., Atlas, t. 162, f. 10. 
 
 + Pal. Indica (Jurassic Fauna of Kutch), i. Ceph., t. 32, f. 2a, 
 t+ Trans. Geol. Soc., v. (2), t. 61, f. 8. 
 
 § Pal. Frang. Terr. Jur. Ceph., i., Atlas, t. 134. 
 
 || Cephalopoden, 1849, Atlas, t. 14, f. 4a. 
 
 “| Trans. Geol. Soc., v. (2) t. 23, f. 8. 
 
 ** Trans. Geol. Soc., v. (2), t. 23, f. 5. 
 
 ++ Pal. France. Terr. Jur. Ceph., i., Atlas, t. 150. 
 
 + Pal. Frang. Ter. Jur. Ceph., i., Atlas, t. 151, 
 
697 
 
 Yet ‘another Ammonite, which Dr. H. Woodward—who was kind enough to 
 examine casts of all these fossils sent him by myself—compares to A. lingulatus, 
 Quenst., of the White Jura. Figures of this species are not accessible to me, and I 
 cannot find anything precisely like it, although it seems to be of the Upper Oolite type 
 of A. Lamberti, Sby., and A. Sutherlandie, Sby., as figured by D’Orbigny,* in so 
 far as the break in the double costation goes, but the back of our shell is much too 
 broad and the coste too fine. The square back, wath its oblique cost, and the 
 marginal crenulations, all convey to this shell a much more Upper Oolite or Lower 
 Cretaceous aspect than they give to it a Lower Oolite facies. Neither is it impossible 
 that a relation may exist between it and 4. Leai, Forbes.+ 
 
 So far as our present knowledge of Queensland Ammonites exists, there is no 
 connection between the latter and either of the species described above, although our 
 one bears some resemblance to Moore’s Ammonites macrocephalust from Western 
 Australia. 
 
 The article then proceeded to refer to the fossils already described as collected 
 by Mr. E. Edelfelt and Mr. T. Bevan, and this portion need not be repeated. 
 
 Such is a brief outline of the Paleontology of New Guinea, so far as it is 
 known to the Writer. Briefly reviewing these facts, it is manifest that the oldest 
 fossiliferous rocks on this Island-continent of which we at present have any record, 
 probably correspond homotaxially with the Upper Oolites of other countries, more 
 particularly the European, at the same time displaying some relation to the Indian beds 
 of the same age. As regards the Inoceramus, it would appear to resemble an old-world 
 Cretaceous species ; but the specimen being a single one, too much stress must not be 
 laid upon this point. It may simply be said that Cretaceous rocks put in a claim for 
 consideration. 
 
 Of the Tertiary fossils it is necessary to speak more fully, but with caution. The 
 presence of Voluta macroptera and V. anticingulata in the Yule Island deposit, would 
 go a long way towards-correlating the latter with the beds containing these shells at 
 Schnapper Point and Muddy Creek, in Victoria, as suggested by Mr. C. 8. Wilkinson. I 
 was indebted to the kindness of the late Prof. W. T. Stephens, M.A., for an opportunity 
 of examining the Yule Island collection in the Macleay Museum,§ but the species 
 mentioned were not observed there, and only those described by the Rev. Mr. Woods 
 came under observation. An attentive examination of these rather leads me to accept 
 Mr. Woods’ suggestions as to the age of the fossils in question. The matrix is also 
 clearly the same as that containing the corals collected by Mr. Edelfelt at Maiva 
 Village. || 
 
 The Urchin described as Zemnechinus does not appear to belong to that genus 
 as defined by its originator, Edward Forbes,4{/ and at the present moment I am 
 not prepared to generically place the specimen. It may probably be an undescribed 
 form. 
 
 The Peronella would appear to be a small individual of the characteristic and 
 generally distributed Australian species to which Mr. Woods has referred it. The 
 
 
 
 * Pal. Franc. Ter. Jur. Geph., i., Atlas, t. 177. 
 
 + Quart. Journ. Geol. Soc., i., p. 178, t. 12a@ and b. 
 
 ~ Quart. Journ. Geol. Soc., xxvi., t. 15, f. 5 
 
 § The fossils were collected by Mr. J. Brazier. 
 
 || Specimens are in the Mining and Geological Museum, as well as in the Queensland Survey Collection. 
 
 §| Mon. Echinodermata Brit. Tertiaries, 1852, p. 5. The New Guinea fossil does not possess the 
 typical excavations along the sutural margins of the plates seen in all true forms of Zemnechinus, nor are 
 the ambulacral plates confluent. These characters are emphasised by Forbes and accepted by A. Agassiz in 
 his ‘‘ Revision.” 
 
698 
 
 specimen of Doliwm costatum, although only an internal cast, is one of so strongly and 
 distinctly marked a species as to be readily recognisable from the other Australasian 
 forms; the simple and distinct cost and canaliculate suture distinguish it at once. 
 The Pecten nove-guinee is not identical, says Mr. Brazier, with any existing species in 
 neighbouring waters, and must therefore be regarded, with the so-called Temnechinus, as 
 peculiar to the Yule Island deposit. It is, however, remarkably like a South American 
 Pecten, described by D’Orbigny? from the Tertiary rocks of Patagonia, as P. paranensis.* 
 In addition to these species just mentioned, I detected in one of the blocks of the 
 Macleay collection the internal cast of a Strombus, which Mr. Brazier regards as that of 
 S. (Gallinula) Campbelli, Gray, a species now living in the Australian seas. 
 
 E. 
 
 
 
 *See Darwin’s Geol. Obs. Vole. Islands and Pts. of 8S. America; Voy. ‘‘ Beagle,” 2nd Edit., 1876, t. 3, 
 f. 30. In P. paranensis, each costa, as in the New Guinea species, is divided into three or four ribs. The 
 concentric lamine in the latter are continuous over the costz and intervening valleys, forming frills, but in 
 the former the ribs of the coste are separately decorated by concentric lines of projecting tooth-like spines. The 
 interior ear also in the South American form is more deeply divided than in our species, and the posterior is 
 less granulate, 
 
 ‘ 
 
CHAPTER XL. 
 
 PETROGRAPHICAL NOTES ON SPECIMENS FROM QUEENSLAND 
 AND ADJACENT COLONIES. 
 
 BY A. W. CLARKH, F.G.S. 
 
 INTRODUCTORY. 
 
 When the following Notes were being compiled I hoped that they would form 
 portion of a larger work, viz.:—The description, in petrological language, of the rocks of 
 Australia ; but want of time, together with the difficulty of getting typical rocks from 
 the other colonies, has narrowed the scope of this ambitious attempt, so that little has 
 really been done besides describing a few of the rocks of Queensland and the 
 neighbouring Colonies. 
 
 As a Queenslander (by adoption), I am glad to be able to contribute, in any way, 
 to the codification of our natural history; and the appearance of these Notes in Messrs. 
 Jack and Etheridge’s Work on the Geology and Palxontology of Queensland is 
 gratifying to me, and not inappropriate, since nearly every rock described in the 
 following pages was collected by the Government Geologist, or by members of his Staff. 
 For the last three years I have constantly been supplied with field notes and reports on 
 these rocks, and am now entrusted with a great deal of the petrological work of the 
 Geological Survey, so far as the preparation of rock-sections is concerned. 
 
 The microscopical drawings, signed ‘‘ J. Pheebe Clarke,’’ were drawn and painted 
 from the microscope by my wife. To those persons who know anything of the subject, 
 they tell their own tale; but for general readers it may here be necessary to describe, 
 as shortly as possible, what they mean and teach. 
 
 Imprimis, the drawings are made from the highly magnified images of extremely 
 thin films of rock. ach film is preserved between two glasses, which are made to adhere 
 together by means of Canada balsam. These films or sections show the exact relative 
 positions of the different constituents of the rock. When they are placed under the 
 microscope, and light is reflected from the sub-stage mirror through the section, the 
 structure or texture of the rock is revealed, and this is a highly important factor in 
 the grouping and classification of rocks. Thus the New Guinea rhyolite, No. 108, 
 drawn on Plate 61, fig. 1, represents fluxion-structure, as do several other of the 
 drawings appended to these Notes. 
 
 In petrological language, “ fluxion-structure’” means that the section bears 
 irrefutable internal evidence of flow during that period of the existence of the rock 
 when its temperature just allowed the creation out of the molten magma of one or two 
 classes of minutely crystalline minerals, which thus become indices of the past move- 
 ment of the rock. 
 
 In examining this particular group of rocks it is easily seen that the microscope 
 plays an important part; for to the naked eye the little lath-shaped crystals seen in the 
 magnified section are generally invisible, while the microscope discovers their presence 
 and arrangement in vast numbers throughout the glassy base, resembling what occurs 
 when a bundle of twigs and straws is cast into a running brook—viz., the twigs and 
 straws arrange themselves end to end in the direction of the flow of the brook. 
 Rocks whose sections reveal, microscopically, this end-to-end arrangement of lath- 
 shaped crystals (crystallites) are placed in the rhyolite group. 
 
 There are other rock structures or textures which are described in various text- 
 books on the subject, and occasionally our own Australasian learned Societies deal with 
 
700 
 
 the subject in their published “ Proceedings.” But the fluxion-structure is the most 
 striking, and it suffices to illustrate, in this particular direction, the value of the 
 microscopical examination of rocks. 
 
 The microscopical examination of its section does more, however, than merely 
 disclose the structure of the rock, for, by using polarized light instead of ordinary light 
 and an avalysing Nicol’s prism (usually referred to as a “ Nicol”), the observer goes 
 further, and is able to identify the different component minerals constituting the rock. 
 
 Tt is hardly possible to explain, in a short introductory chapter, how this is 
 done; but, to simplify the matter so that general readers may be attracted to, and not 
 repelled from, what is really a most attractive subject, 1 will try to explain how 
 polarized light differs from ordinary light. 
 
 If we imagine a ray of ordinary light to be magnified many millions of times, 
 then that portion of a test-tube cleaner which carries bristles, or the same portion of the 
 cleaner supplied with an infant’s feeding bottle, may represent, roughly, the ray of 
 ordinary light, the wire being the path, and the bristles representing the cross vibra- 
 tions of the ether-particles. By arranging the bristles parallel to each other a fair 
 illustration is obtained of the polarized ray. 
 
 Thus, then, in ordinary light, the ether-particles vibrate in all directions across 
 the path of the ray ; and in polarized light, the ether particles vibrate in parallel planes 
 across the path of the ray. 
 
 Now, to produce polarized light we can compel the ether-particles to vibrate in 
 parallel planes, in two ways—either by reflection from glass or polished metallic surfaces, 
 at certain angles, dependent on the nature of the reflecting material; or by refraction 
 through crystal plates. Nicol (a Scotch professor) found out how to obtain this polarized 
 light by compelling it to pass through prisms of Iceland spar (a variety of calcite), 
 specially cut and prepared; and this is the method universally adopted in petrography 
 at present. 
 
 To recognise when light is polarized requires a similar prism or reflecting plane. 
 Hither does, no matter what means are employed for polarizing the light to be examined. 
 
 In the microscopes used for petrographical work there is a polarizing prism 
 beneath the stage, and a precisely similar prism over the eye piece. Both can be revolved ; 
 and by adjusting the analysing prism so that its principal axis is at right angles to that 
 of the lower polarizing prism, perfect darkness covers the field of the microscope, and 
 the nicols are technically known as “ crossed.” 
 
 By turning the analysing prism the field gradually gets illuminated till at 90° 
 the maximum of illumination is reached, and the nicols are said to be “ parallel.” A 
 continued revolving of the analysing prism would lead to the gradual darkening of the 
 stage until no light passed through, when the nicols would be again “ crossed.” 
 
 Most of the drawings illustrating these Notes represent sections as viewed between 
 crossed nicols, and under such circumstances the different minerals exhibit characteristic 
 optical properties. For instance, the bands appearing in one of the minerals in the drawing 
 of the Cape Upstart section certainly prove it to be one of the felspar group of minerals. 
 Again, colour is of some value, certain minerals being illuminated vividly, like the augite 
 crystal depicted on Plate 65, fig. 2; while orthoclase is always a delicate lavender grey. 
 These colours vary, however, being dependent on the thickness of the section. 
 
 There is one system of crystals belonging to the cubic form and its derivatives, 
 none of which are illuminated at all, even in thick sections.* To this group belong 
 fluorspar, garnets, &c. They are, therefore, easily recognised. 
 
 
 
 * A thin section may be about ‘001 inch or less, while a thick section would be about ‘006 inch or 
 even thicker. 
 
701 
 
 Finally, to render this introductory preface as complete as possible, I will briefly 
 describe the method of preparing rock-sections. 
 
 Sorby * (one of the fathers of petrography) prepared his sections by grinding a 
 flake of the rock and polishing it on one side.t The polished surface is next cemented 
 with Canada balsam to a piece of plate glass, which latter forms a sort of handle, 
 as well as insnring more or less parallelism between the two faces of the polished 
 film. The best grinding surface is plate glass with a sprinkling of emery powder 
 (No. 40); and for polishing, I always use flour emery, on another and similar glass 
 plate. The powders are kept fairly moist with water. The rough side of the mounted 
 flake is then ground down till a mere film of rock remains adhering to the glass. 
 That film is the “section.” When properly ground it is in most cases perfectly 
 transparent—hornblende transmitting green light; quartz, white light; and felspars 
 being more or less transparent, according to the changes that the rock may have 
 undergone. 
 
 Different students have, of course, different methods of working. I use a 
 lapidary’s wheel, which facilitates the work ; but the simplicity of the other apparatus 
 commends itself to a frugal mind. 
 
 Having then obtained a film of rock containing various contiguous minerals, the 
 thickness of which may vary between ‘006 inch to ‘001 inch, we proceed to mount it in 
 Canada balsam, and then to examine it according to the methods detailed in the above 
 sketch. In this way, a rock-section, when carefully prepared and examined, reveals to 
 a trained eye different contiguous mineral films. The structure and texture of the 
 aggregate is first noted; next the minerals are examined for their optical properties, 
 which are compared with the tabulated optical constants of rock-forming minerals, and 
 thus identified. 
 
 Lastly, under a high power, t-inch or }4-inch objective, the gases, liquids, and 
 solids included in the different minerals are observed. Under such a power quartz 
 reveals vast masses of gas-bubbles aud liquids with little oscillating bubbles. These 
 bubbles go on travelling round the walls of their tiny prisons apparently for ever ; and 
 in one section, ‘001 inch thick, literally scores of these enclosures can be seen between 
 the two polished surfaces of the section. In one of Fuess’s sections under ‘001 inch 
 thick, belonging to Mr. Jack, I have counted over ten almost superimposed, yet never 
 touching each other, and with room for a score or so more, in each of which the little 
 bubble flew round.t In this particular section there were over 1,000 enclosures in every 
 cube whose edge measured ‘001 inch, and this was by no means a quartz rich in 
 enclosures. Quartz is not the only mineral exhibiting such phenomena. 
 
 In concluding these few Notes, introductory to the science of petrology and 
 petrography, I will leave the general reader to form what judgment he can on the 
 microscopic structure of some of our Queensland rocks, asking pardon from students 
 of geological science for my temerity in writing such a bald introduction to so vast a 
 subject. 
 
 A. W. CLARKE. 
 Charters Towers, 26th June, 1892. 
 
 
 
 * H. C. Sorby, F.R.S., late Pres, Geol. Society. 
 
 + Mr. W. H. Rands, F.G.S., Assistant Government Geologist, obtains excellent flakes by smashing, 
 with a vigorous blow from a sledge hammer, a large lump of the rock ; amongst the débris, Mr. Rands states 
 that generally several suitable flakes will be found. 
 
 + Mr. Jack informs me that these sections have been in his possession for more than sixteen years ; 
 and yet they stz// show the oscillation, 
 
702 
 
 NOTES. 
 SS 
 GRANITES. 
 
 No. 26. Kitna of Croypon Cram, Croypon (QUEENSLAND). 
 R. L. Jack’s Collection. Sp. Gr. 2°661. 
 
 Colour red. Granular, allotriomorphic. Water-clear quartz, reddish felspars, 
 hornblende sparse, with magnetite, epidote, and ferrite as secondary minerals. 
 
 Quartz clear, allotriomorphic, with numerous inclusions ; some rather large with 
 moving and fixed bubbles, the latter unaltered by exposure to ice, or a jet of hot air 
 blown on to the section through a blowpipe whose tube was heated with a small spirit- 
 lamp while the slide was on the microscope stage. A few long clear fine prismatic 
 needles penetrate the quartz in no particular direction, in some cases passing through 
 the quartz into a neighbouring felspar. Their index of refraction must be high, for 
 the needles shine out sharply with dark borders. I think they are rutile, which Teall 
 suggests as occurring in the quartz of some of the Scotch granites ; only he describes 
 them in a single word as being “ hair-like,”’* while these needles are not trichitic. An 
 actual measurement (with a Stage Micrometer, however) gave ‘03 x ‘0005 inch. 
 Ferrite is enclosed in the quartz, amorphous, visible under the 4-inch objective. With 
 the ferrite occur flecks and specks of what must be hematite, being bright orange-red 
 and transparent to translucent, but they are found more in the irregular cleavage-cracks 
 and fissures, pointing to secretion, from pre-existent minerals, carried on for ages by the 
 infiltration of water. 
 
 Felspars much altered, nearly opaque. They enclose dirty light-green epidote. 
 Magnetite occurs once only, associated with possible epidote and chlorite, in the wreck 
 of a plagioclase felspar. In ordinary transmitted light there appear long parallel cuts, 
 allowing the light to pass up through a semi-opaque mass of dusty and cloudy matter. 
 Between crossed nicols, these lines are parallel with an axis of extinction. Whether 
 this is due to the “ aggregation of a perfectly uniform colourless substance along the 
 cleavage-cracks of an orthoclase erystal,’’ as noted by Rosenbusch,* I cannot say. The 
 structure is common in the felspars of Croydon and Charters Towers, and among other 
 granites. 
 
 Hornblende brown, showing cleavage parallel to C, generally fringed with epidote. 
 If the hornblende abuts on quartz and felspar the epidote prefers, invariably, to secrete 
 itself on the felspar side. A few instances of the fan-shaped groups of epidote occur, 
 as drawn in Zirkel’s Petrography.t - ° 
 
 No. 162. Ernrertpar Gorp Frerp (QUEENSLAND). 
 R. L. Jack’s Collection. Sp. Gr. 2°615. 
 
 Colour greyish white. Granular, with large fresh idiomorphic felspars, often 
 $-inch long, with well-marked cleavage. 
 
 Quartz allotriomorphic, and the whole speckled with small grains of biotite. 
 Very little hornblende. Both biotite and hornblende are accessory minerals. 
 
 
 
 * J.J. Harris Teall. British Petrography, 1888, p. 324. 
 
 + H. Rosenbusch. Microscopical Physiography of the Rock-making Minerals, translated by Joseph 
 P. Iddings, 1888, p. 286. 
 
 {Ferdinand Zirkel. Microscopical Petrography, in Report Geol, Explor, Fortieth Parallel 
 Washington, 1876, Plate iii., Fig. 4. 
 
703 
 
 Felspars frequent and fairly fresh, consisting of orthoclase, microcline, and 
 plagioclase. The first is the least’fresh, and often there is an intergrowth of the first 
 two mentioned. The microcline is exquisitely lined, markings under the }-inch being 
 finer than the finest lines in a good steel engraving. ‘The simultaneous extinction of 
 the two sets of cross lines is marked; one set of cross lines is less perfect than the 
 other, being slightly spindle-shaped or wedged. The angle between the two sets of 
 lines varied between 91° 30’ and 93°, but it is not easy to see when the cross web exactly 
 coincides with the less regular cross lines of the felspar, so that the angle in no case is 
 quite accurately measured. In the plagioclases the angle between the traces of the 
 twinning planes and an axis of elasticity is between 7° and 10°. In one case the 
 angles of extinction on either side of the twinning planes were 8° 10’ and 7° 30’—angles 
 so nearly equal that it will be safe to assume that the section of the crystal is cut parallel 
 to the zone at right angles to MZ. The nearest angle to the mean of these given in 
 Rosenbusch* is 7° 35’, which would give a formula to these felspars of Ab* and An‘.+ 
 
 Quartz rich in inclusions and microlites. The inclusions are sometimes fluid and 
 dihexahedral, with moving bubbles. The microlites are an interesting feature in the 
 rock, as they closely resemble those in the quartzes of granite found at Summit 
 Springs, Hovallah Range, North America, described and drawn by Zirkel ; but he 
 describes them as being black, whereas the microlites in the quartzes of my section are 
 milk-white by reflected light, strongly resembling the raphides found in Typha 
 angustifolia, Linn.,t except that the microlites much exceed the raphides in length. 
 
 The quartzes do not always polarize uniformly, and may be described, according 
 to Professor Hutton’s nomenclature of rock textures, as granulitic.§ 
 
 The Mica is a dark-brown biotite, and very sparsely distributed. 
 
 No. 14. Cooktown (QUEENSLAND). 
 F. Bauer’s Collection. Sp. Gr. 2°6437.|| 
 
 Colour grey. Granular, allotriomorphic. Felspars large, commonly 4-inch and 
 sometimes 3-inch long, idiomorphic, cleavage well-marked when held in light falling 
 onit obliquely. Sparsely scattered allotriomorphic quartz. Little hornblende. Biotite 
 and tourmaline in minute black shining grains and prisms. 
 
 Quartz rich in inclusions, varying considerably in size, a few just visible under 
 the 1-inch objective; some fluid, with moving bubbles ; others with fixed gas pores, also 
 glass inclusions. They are all spread out in planestraversing the crystal and crossing each 
 other at low angles. The more persistent are rudely parallel to an axis of elasticity, 
 possibly the principal axis. The micrometer screw shows how they “hade”’ in all 
 directions. What I take to be the glass-inclusions are very irregular in outline, being 
 pear-shaped, globular, and quite irregular, resembling the smear left by an oily finger 
 on perfectly polished glass or the magnified image of a finger-mark on a glass-slip such 
 as is used for mounting microscopic objects. 
 
 Felspars much decomposed, showing the clear, straight lines described in the 
 Croydon granite, No. 26 (probably orthoclase). 
 
 
 
 * “ Microscopical Physiography,” p. 300. 
 
 + Where Ad represents albite, and An anorthite. Vide note at end of Chapter. 
 
 + A bulrush infesting tailings-dams at Charters Towers. Sce ‘‘Synopsis of the Queensland Flora,” by 
 ¥. M. Bailey, p. 571. Brisbane: by Authority : 1883. 
 
 § Prof. Hutton’s Catalogue of Rock Textures, as given in his Paper, on ‘‘The Eruptive Rocks of New 
 Zealand.” (Proc. R. Soc. N.S. Wales, 1890, xxiii., p. 107.) 
 
 || In determining these Sp. Grs., as large a piece of rock as could be procured has always formed the 
 material for experiments. The piece used in this determination weighed 18,189 grains, which warrants 
 carrying the calculation to the 4th decimal place. This rule has been observed throughout, 
 
 * 
 
704 
 
 Tourmaline is in short stunted prisms, very pleochroic, varying from red, pink, 
 yellow, and green to blue. Often the tourmaline is in rounded grains. 
 
 Biotite in hexagonal brown plates, very small. No magnetite, and very little 
 apatite. : 
 CooKTowN (QUEENSLAND). 
 
 A. J. Madden, Esq., Collector. 
 
 Tourmaline and cassiterite associated with quartz. 
 
 Although this aggregate of minerals has no place amongst the granites, it comes 
 in with some advantage here, because Plate 63, fig. 2, illustrates a tourmaline crystal in 
 quartz from the same Cooktown district. The tourmalines drawn on the plate show the 
 pleochroism and the cleavage of the microscopic tourmalines in the Cook district. The 
 section was prepared from a piece of quartz-carrying cassiterite and tourmaline, forming 
 part of a large sample of tin ore sent for assay by A. J. Madden, Esq., of Cooktown. 
 The exact locality is not known to me. The ore is typical of over a hundred samples 
 assayed by myself from time to time from the neighbourhood. The tourmalines tend 
 to separate into segments transverse to the principal axis (¢.e., along the cleavage), quartz 
 filling up the spaces left. The quartz so introduced between the segments “ orients” 
 uniformly with that contiguous to the sides of tourmalines. The quartz does not 
 always uniformly polarize, however; much of it is in the form of granulitic aggregates. 
 These aggregates often, but not always, border large grains of ‘quartz, separating it from 
 its neighbours. In these quartzes the tourmalines pass through larger grains and 
 aggregates, sometimes being separated into segments in the larger crystals, and at 
 others in the suture. 
 
 The interesting question arises, which of the two minerals is the first born. 
 Rosenbusch says* that “ tourmaline is not directly secreted out of the eruptive magma 
 in eruptive rocks, but resulted from the action of fumaroles, carrying fluorine and 
 boron, on the eruptive rock, especially on its felspar and mica.’ Teall also alludes to 
 the action of fumaroles in the genesis of tourmaline. This would rather support the 
 pre-existence of the quartz. On the other hand, the uniform orientation of the quartz - 
 between and alongside of the broken prisms would lead one to think that the 
 reverse was the case. Could it be that the tourmaline crystallised out in the 
 quartz by the action of fumaroles, as above, while the quartz was viscous and under 
 pressure, and that earth-stresses and dynamic metamorphism followed, separating the 
 prisms, after which the quartz proceeded to crystallise P+ 
 
 Cassiterite isin brown, gum-like drops, sometimes honey-yellow, included between 
 tourmaline prisms. 
 
 Quartz very dusty and, under the 4-inch objective, shows yellow, yellowish-red, 
 and red flecks, probably hydrated oxides of iron. The inclusions are very numerous, 
 but exceedingly minute. Some are liquid; others might be liquid with gaseous 
 envelopes, but this has not been definitely ascertained. Certainly some of the inclusions 
 contain oscillating bubbles only visible under the $-inch. In all of the section prepared of 
 this rock or sample of tin-bearing quartz, the tourmalines were sharp and highly 
 
 
 
 
 
 * 
 
 ‘Microscopical Physiography,” p. 184. 
 
 + Since these slices were prepared Mr. Jack has shown me a most striking example of the parting of 
 tourmaline in quartz, the quartz having filled up the spaces between the segments just as in the above 
 samples, but the evidence of dynamic metamorphism is much more striking in this sample (which comes 
 from the same district, and, I strongly suspect, from the same mine). Mr. Jack’s specimen shows how the 
 tourmaline has also been bent out of the straight, small bundles of the prisms following the curve. The 
 bundle of tourmaline crystals forms a flagellum about four inches in length. The specimen came from the 
 Mount Leswell Tin Mine, Cooktown. 
 
705 
 
 crystalline. The edges of the partings are still jagged, when highly magnified (4-inch 
 objective), as they were the day they separated. On the other hand, the tourmaline 
 in the Cooktown granite is highly granular, and the small prisms by no means sharp. 
 
 No. 250. Movnr Brsmancx, CoongarRa (QUEENSLAND). 
 A. G. Maitland’s Collection. Sp. Gr. 2°66. 
 
 Colour, dark-brown. Fine-grained, almost microgranitic. Quartz, hornblende, 
 with epidote in grains, plagioclase and orthoclase. 
 
 Section.—Quartz is hardly granulitic, owing to the epidote, which is interstitial. 
 But for this it would fulfil the definition—viz., “ In approximated allotriomorphic grains, 
 small, of nearly the same size, and independently oriented.” 
 
 Rare mica; in one case it is fibrous, much broken up into septe between 
 crossed nicols, the ends of the fibres frayed out, the whole slightly curved in the form 
 of the letter S. 
 
 No apatite or magnetite. 
 
 No. 257. Drrwenr Creex, Coongarra (QUEENSLAND). 
 A. G. Maitland’s Collection. Sp. Gr. 2°718. 
 
 Colour, dirty red. These rocks are not true granites, and, according to Professor 
 Hutton’s system, would be placed in the elvanite group, as they consist of microgranitic 
 orthoclase and quartz, with porphyritic crystals of quartz and orthoclase, and sparsely 
 distributed hornblende, or perhaps mica. 
 
 Section.—The quartzes are generally allotriomorphic, and often the felspar and 
 quartz are in a crystalline-granular state—pegmatitic (graphic-granite). Rutiey would 
 probably class these two rocks as haplites. The pegmatitic quartzes carry the usual 
 inclusions, but they are minute, and a great many are mobile. The inclusions are not 
 arranged in lines, but occur without system, and, as it were, haphazard; while in the 
 porphyritic quartzes the inclusions’ are arranged much more systematically, being 
 generally strung together in lines, which, however, bear no constant relation in their 
 direction to the crystallographic or any other axis. 
 
 The felspars are finely fibrous. One single example occurs of plagioclase. It is 
 too much altered to classify, but it is distinctly banded ; and the angles of extinction, right 
 and left of the twinning planes, are—right, 10° 40’; left, 15° 30’. 
 
 The fibres cross at an angle of 46° 30’. Some of these fibre-spectra cross each 
 other at right angles, and are suggestive of microcline, but the felspars are all so opaque 
 that their optical properties are not discernible with any precision. Unfortunately, in 
 the three slices beside me of this rock, the hornblende or mica isabsent. One or the 
 other, however, occurs, or perhaps both may occur, as accessory minerals visible to the 
 naked eye, in the hand specimeus. 
 
 No. 255. Derwent Creek, CooLgarra (QUEENSLAND). 
 A. G. Maitland’s Collection. Sp. Gr. 2°568. 
 
 Colour, a dirty grey, with ill-defined dirty green specks of secondary origin. 
 The same remarks apply to this rock as to No. 257, except that some ferrite occurs, 
 and a little epidote around very minute hornblendes. 
 
 2w 
 
706 
 
 No. 188. Homestrap Rance, Norruern Rattway (QUEENSLAND). 
 
 W.H. Rands’ Collection. Sp. Gr. 2°58. 
 
 Colour, red. Would be placed by Professor Hutton in the same class as Nos. 
 255 and 257. 
 
 Orthoclase is the prevailing felspar. Sometimes the latter is quite clear and 
 limpid. The kaolinized felspars are stained red with oxide of iron, and sometimes 
 ferrite is concentrated round centres, the eyes of which are opaque, the edges being 
 transparent and just stained. 
 
 Section—Micropegmatite occurs, showing the simultaneous extinction of the 
 interpenetrating quartz when the section is revolved. The quartzes contain the usual 
 fixed and oscillating bubbles. The micrometer-screw reveals planes formed of extremely 
 minute inclusions which have a faintly pink tinge to my eye, and are transparent. The 
 inclusions are probably glassy. Sometimes their shape is similar to that of the inclusions 
 described as occurring in quartzes in the Cooktown granite, but more often they are 
 round or ovate; the smallest would measure less than ‘0001 inch. The micrometer- 
 screw shows how they traverse the crystal in various planes, whose directions are 
 independent of any of the crystal axes. The quartz, when porphyritic, is often idio- 
 morphie, as is also the orthoclase. Macroscopically, the rock carries sparse black specks, 
 which have not been determined. 
 
 No. 202. Norru or Curnaman’s Guuty, Care River Gotp FIeEtD (QUEENSLAND). 
 
 W. H. Rands’ Collection. Sp. Gr. 2°663. 
 
 Colour, nearly white. Quartz, white mica, felspars, and garnets, the latter pale 
 yellow. The structure is granular, granitic, or holocrystalline, and the minerals are all 
 fresh and transparent. 
 
 Section.—The felspars are most abundant, and therefore come first. One felspar 
 is much kaolinized, but still sufficiently fresh to identify. 
 
 The axes of extinction, on either side of well marked cleavages, are—right, 
 7° 20'; left, 8° 50’. The cleavage being so well marked, and the angles of extinction 
 with regard to it being also well marked, show that the section is probably cut parallel 
 to the plane of symmetry 010, and the cleavages must be parallel to the basal pinakoid, 
 all pointing to orthoclase which is rather fresh. In addition, there are plagioclase 
 felspars, some very finely striped and others coarsely striped, suggestive of oligoclase. 
 
 The mica is a potash mica, and possibly muscovite. The sections show marked 
 absorption for rays vibrating parallel to the basal planes in such crystals as are cut 
 transverse to the lamelle. 
 
 The garnets appear brilliant and rough, of course, by reflected light, owing to 
 their high index of refraction. Their optical properties are normal, and irregular cracks 
 traverse the crystal. The grains average ‘01 inch in diameter, and are of a pale-yellow 
 pink colour. Probably they are almandine garnets. The inclusions in the quartzes 
 are very small, being only just discernible under the 74-inch objective, and under the 
 $-inch a few minute moving bubbles were to be seen. 
 
 Nos, 240, 241, 242, 243. Vicrorta Reer, Coarters TowErs (QUEENSLAND). 
 These rocks were collected by the Hon. H. Mosman, M.L.C., with the view of 
 determining, through Professor Judd, whether there is any difference between granite 
 bordering gold-bearing reefs and granite bordering non gold-bearing reefs. The four 
 samples were sectioned in my laboratory ; and before their despatch to Professor Judd, 
 
707 
 
 Texamined them. Nos. 240 and 241 are from the hanging and foot walls respectively of 
 gold-reef-bearing granite ; while 242 and 248 are the hanging and foot walls of the 
 non-gold-reef-bearing granite. 
 
 Macroscopically, the specimens are grey. No. 240 is permeated by one single 
 vein, ~; inch thick, of # zeolite, which I have often analysed, as per Mineral 
 Census, Royal Society, Queensland, &. Vide Plate 67, fig. 2. The rock consists 
 of quartz, felspars, and hornblende. There is no mica visible with a lens in the hand 
 specimens. 
 
 Section.—The texture is granitic, holocrystalline. The richness of the quartzes 
 in fluid-inclusions is very great. Planes of these inclusions intersect in various 
 directions, and each plane absolutely teems with fluid-inclusions. Under the one-inch 
 objective, by oblique reflected light, these inclusions appear beautifully silvery. The 
 hornblende is bright green, in part often crumpled, and sometimes reedy (the “schilfige 
 hornblende” of Rosenbusch). 
 
 Well-defined crystals of magnetite appear, both included in this hornblende and 
 on the margins. The magnetite occurs in the felspars when remote from hornblende, 
 and in one case the octahedral crystal is in quartz, having been derived from the horn- 
 blende which is contiguous to the quartz, but this is uncommon. All these exhibit 
 strong magnetism on powdering and washing off the dirt, and using the magnetised 
 needle as a means of separation. In the neighbourhood of magnetite crystals, 
 exquisitely clean-cut apatite crystals aggregate, as is the habit of this mineral. In a 
 prism of apatite, ‘008 inch long and ‘OOL inch broad, there is a fluid-enclosure whose 
 figure is symmetrical with its host. 
 
 The hornblende is frequently interpenetrated by epidote of a yellowish-green 
 tint, polarizing in high colours, and appearing, by reflected light, very rough on the 
 surface, owing to its strong index of refraction. The pleochroism of the hornblende is, 
 for rays vibrating parallel to cleavage, bluish green, and at right angles itis yellow. In 
 many crystals the cleavages are parallel to an axis of elasticity. 
 
 Felspars.—They are much altered, probably orthoclase amongst them, but not 
 certain, and in small quantity. The section must be fairly thin, since the quartzes only 
 colour to No. 13 in Newton’s scale, and sometimes lavender grey, yet the great majority 
 of the felspars are filled with a perfectly transparent colourless mineral, which is strongly 
 coloured between crossed nicols. From the fan-shaped groups of some of these invested 
 secondary secretions, it is probable that they are epidote. Some may be calcite. In 
 No. 241 orthoclase occurs sparingly and between crossed nicols; the felspar is not 
 simultaneously extinguished on turning the stage. A black envelope environs a 
 luminous centre, and that is succeeded by a luminous envelope environing a black 
 centre (7.e., “ undulose extinction’’). 
 
 There is a curious affinity between the magnetic iron and the apatite. Very 
 little difference exists between the hanging-wall of the gold-bearing quartz and the 
 hanging-wall of the non-gold-bearing quartz. In No. 242 there appears perhaps iess 
 hornblende than in No. 240, and what there is, is more crumpled. In No. 243, the 
 felspars are less kaolinized, and orthoclase twinned on the Carlsbad type occurs together 
 with plagioclase. One large orthoclase crystal shows signs of zonal structure, and 
 exhibits undulose extinetion. 
 
 “In No. 242 the felspars are most delicately banded, and the hornblende is 
 crippled, while the other parts of the slide can be described as in the foregoing cases. 
 Some of the felspars in No. 240 appear like picture frames with much beading, slightly 
 thrust on one side-—7.e., like quadrilateral figures with their opposite sides equal, but all 
 their angles not right angles. 
 
708 
 
 Werriineton Reer, Cuarrers TowErs (QUEENSLAND). 
 From 600 feet vertical depth. Portion of core from diamond drill. 
 
 Section.—Quartz shows fewer and smaller inclusions, sometimes very minute 
 and red (hematite probably). Epidote and magnetite as before. A little apatite, but 
 less than in the four previous rock samples ; orthoclase and microcline, the former 
 being often filled with fine particles of mineral matter polarizing in high colour. Vide 
 Rosenbusch on “‘ Epidote.” * 
 
 The other felspars are much decomposed and difficult to identify. The orienta- 
 tion in most of the felspars is undulose. This was the first of a series of rocks that I 
 sliced in Charters Towers, and is hardly thin enough for microscopic examination, the 
 quartzes all polarize in a deep purple colour, owing to this, whereas in the previously 
 described samples from Charters Towers, the quartzes are all light yellow or lavender. 
 
 The hornblende is much replaced by minerals of secondary origin, viz—epidote, 
 chlorite, magnetite, and viridite. 
 
 Norrnh Avstrattan Reer, Cuarrurs TowErs (QUEENSLAND). 
 
 From deep ground. 
 
 The special characteristic of this rock is the very large amount of hornblende 
 present. Unfortunately I have only the slice, which is too thick, as it belongs to a 
 group of rocks similar to the preceding. 
 
 There are two varieties of hornblende, a grass-green species with feeble 
 absorption for rays vibrating parallel to an axis of elasticity. Then there are some 
 granules with very irregular outlines, whose greatest length and breadth would not 
 exceed ‘91 inch, whose pleochroism is very marked, ranging through green, yellow, and 
 rose-pink to red, in the course of a quarter revolution of the stage. At one position of 
 the stage the centres will be surrounded by zones of different colours. These, from 
 the high refractive index, should be epidote. The other species of hornblende is brown, 
 showing well-marked cleavages, with an angle of extinction of 14° 40’ to these cleavages. 
 In other examples of the hornblende the extinctions with regard to cleavage, fall to 0°. 
 Absorption very strong for rays vibrating parallel to cleavages. The felspars show a 
 high angle of extinction (—29° 40' on P.) Therefore there must be much anorthite 
 present, as indeed is shown in the following partial analysis of a Charters Towers 
 granite published in the Annual Report of the Mines Department for the year 1887.+ 
 The sample is from the Court-house Reserve, and was dressed up from a boulder at 
 surface. The sample looked quite clean, and was not perceptibly weathered. 
 
 Silica... ba a ae of oi ... 72°00 per cent. 
 Iiyesey ss fue ni 500 oes sa aos 
 
 Alumina wae a on wa ate 500 aes 
 fame,-CaQ" iz. my a af mae wae 3°22 i 
 Loss on ignition ire ht a ry sc BO Ee 
 
 The iron and alumina together present in the sample weighed over 20 per cent. 
 No attempt was made to ascertain whether the iron was protoxide or ferric oxide. 
 
 The felspars are twinned on the albite and pericline law, and often highly 
 kaolinized. Orthoclase rare. . : 
 
 The quartzes are full of inclosures, and the same description given in Nos. 240 
 to 243 applies here. 
 
 
 
 
 
 * *€ Microscopical Physiography,” p. 286, 
 + Brisbane: by Authority : 1888, 
 
709 
 
 Microliths, probably of hornblende, occur, and apatite often penetrates the 
 hornblende, and is easily recognised by its glaring limpidity, and when cut transversely 
 on o P the crystal sections are, of course, hexagonal and isotropic. 
 
 Magnetite occurs as in other Charters Towers rocks. 
 
 Court Hovsrt Reserve, Cuarters Towers (QUEENSLAND). 
 
 Surface boulder, weighing several tons 
 
 Is very similar to the last, except that, being a surface stone, nas suffered from 
 weathering, the result of which is that there are few minerals fresh enough to be of 
 much interest, except the quartz, which is exceedingly rich in fluid and gaseous inclu- 
 sions. Magnetite abounds. 
 
 The triclinic felspars show marked cleavage, rectangular to the striations; and 
 the orthoclases show striz. Tbe minerals of secondary origin are similar to the other 
 Charters Towers samples of granite. 
 
 Unirep Queen Consors Reer, Cuartrers Towrrs (QUEENSLAND). 
 
 “Deep ground.” 
 
 Differs from the North Australian sample in the sparseness of hornblende and 
 its derivatives. 
 
 The constituents are granular qnartz and felspars, with an occasional prism of 
 actinolite. The rock sometimes has blade-like crystals of green actinolite, two or three 
 inches long. The felspars are like those occurring in the Cooktown granite, No. 14 
 showing the white ruled surface by reflected light, the ruled lines being transparent by 
 transmitted light, and being extinguished parallel to the principal section of the polarizer 
 between crossed nicols. 
 
 A little chlorite showing feeble absorption. No epidote. Magnetite, or apatite, 
 and the felspars and quartzes, as a rule equal in size, measuring ‘01 inch. 
 
 No.6. Star River (QUEENSLAND). 
 R. L. Jack’s Collection. Sp. Gr. 2°69. 
 
 Colour, dark-grey. A medium-grained rock with quartz, felspar, and black mica 
 (biotite) in fairly equal proportion, and a little hornblende. 
 
 Section.—By reflected light, pure milk-white felspars, other limpid felspars, 
 clear quartz, and dark mica, some black-lustered mineral enclosed in mica and a very 
 little light greenish brilliant epidote. 
 
 Felspars.—Some of the triclinic felspars are exquisitely marked, the crystals 
 being fresh and the bands extremely fine and sharp. - The finest in the slice is ‘08 inch 
 long by about ‘027 inch broad.* There are twenty-two parallel lines, whose extinction 
 right and left of the normal to the twinning plane JZ is 6° and 6° 10’, respectively, so 
 ‘the section must be about exactly normal to the twinning plane. Another felspar gave 
 22° 10’ and 22° 30’ on either side of the boundary lines between the lamella. Some of 
 these felspars are not uniform in their orientation, and some of the orthoclases show 
 zonal structure. The inclusions in the plagioclases are numerous; some consisting of 
 clear, colourless, rounded grains; and others similar, but green. With these are black 
 opaque grains, probably magnetic iron, also trichites. The orthoclases are very dusty, 
 with possible kaolin. The hornblende fringed with epidote in places, sometimes highly 
 
 
 
 * None of my microscopic measurements are exact, as they have been determined with a stage 
 micrometer, 
 
710 
 
 pleochroic, showing bright green, red, and yellow. Some of the hornblendes are 
 pierced with apatite, its hexagonal section looking like holes. Some of the hornblende 
 has a highly pleochroic tip or teather-edge, which for light vibrating parallel to the 
 cleavage, is reddish-yellow, and at right angles, blue. Many microliths of hornblende 
 in the quartz. 
 
 The quartz is not plentiful, but is allotriomorphic, full of small inclusions and 
 microliths, much traversed by planes of inclusions, a few with very dark margins 
 pointing to gaseous, a few mobile pointing to fluid, and a few sporadic, probably glass, 
 and a vast quantity of dusty particles. 
 
 The mica is probably biotite, often pierced by apatite. 
 
 Magnetic generally contiguous to the hornblende, and in the neighbourhood of 
 apatite. The apatites are larger than usual, measuring about ‘001 x ‘002 inch. 
 
 No. 77. Kipper Pornt, Mount Exriorr, near TowWNSVILLE (QUEENSLAND). 
 
 R. L. Jack’s Collection. Sp. Gr. 2°628. 
 
 Colour, reddish-brown. 
 
 Felspars, quartz, mica, and hornblende. Microscopically there appears to be 
 more felspar than all the rest added together. Felspars orthoclase twins, Carlsbad 
 type, rather altered, showing bright lines as described in the Cooktown and Etheridge 
 granites, often interpolating felspars of the albite and oligoclase type with somewhat 
 broad lamellae. 
 
 The rock derives its reddish-brown tint from the oxide of iron which stains the 
 orthoclase. ~ Plagioclase, very fine, large, the crystals delicately cross-hatched, Jooking 
 like the plan of a building, but not quite rectangular. In the centre of these rhom- 
 bohedral figures are inclusions of ferrite, hematite, apatite, and dusty matter. 
 
 The apatite is plentiful and ranges in size from ‘005 inch across the section of 
 prism to ‘0005 inch, and these latter are sometimes ‘04 inch long. Amongst the colonies 
 of apatites are generally to be found greenish hornblende and magnetite. Epidote is 
 rare. 
 
 Quartz sparse, containing the usual inclusions, which, however, appear fixed, and, 
 from the dark borders, may be glass. The quartz seems to be peppered with dusty 
 particles and glassy inclusions. 
 
 No. 76. Magnetic Istanp, NEAR ToWNSVILLE (QUEENSLAND). 
 
 R. L. Jack’s Collection. Sp. Gr. 2°641. 
 This rock is similar in every respect to the preceding, except that it appears 
 more weathered, and perhaps carries more hornblendes. It obviously belongs to the 
 same series. 
 
 No. 25. Mount Catuerine, St. Hetens, neAR Mackay (QUEENSLAND). 
 
 A. G. Maitland’s Collection. Sp. Gr. 2°64. 
 
 Colour, grey. Fine-grained, no mineral large enough to identify without a lens, 
 microgranitic, holocrystalline. 
 
 Section.—By reflected light, lath-like milky felspars; green hornblende, the 
 larger sections of which are pierced with pellucid apatites which shine like diamonds ; 
 biotite in grains; and but little quartz; the whole section literally peppered with 
 magnetite. 
 
711 
 
 Felspars.—About three-fourths of the section is made up of the lath-shaped 
 felspars, which are opaque, even on the edges of the section which is always the thinnest 
 part, being feather-edged. One much altered felspar shows the fine striz in the centre, 
 but it becomes lost on the margins, where the kaolinization has effaced it as a felspar. 
 Another felspar *1 inch long, is very clear, and for a portion of its length is nearly 
 ‘015 inch broad, and shows the traces of twinning plane Jf very clearly. Quartz, crossed 
 by very pale, slender needles, probably hornblende, inclusions unimportant and sparse. 
 Hornblende well marked when cut parallel to o P, showing cleavages crossing at the 
 angle of about 125°. Magnetiteabounds. The larger particles, however, are found more 
 often in the neighbourhood of the hornblende, associated with apatite. Biotite showing 
 marked absorption for the rays vibrating parallel to cleavage. When cut parallel to 
 the base they are difficult to identify, owing to their granular state. A little pyrites in 
 minute cubes in the powder when panned off. 
 
 No. 74. Mackay (QUEENSLAND). 
 
 A. G. Maitland’s Collection. Sp. Gr. 2°68. 
 
 Colour, dark greyish-brown. Highly felspathic, hornblende, and very little 
 quartz. 
 
 Section.—The bulk of this rock is make up of triclinie felspars, ‘07 to ‘1 inch in 
 length. Originally, these felspars must have been extremely beautiful—even now the 
 striations are exquisitely regular when not marred by kaolinization. 
 
 In one mass of twins there are ninety-three lamelle, broken here and there by 
 opaque secondary minerals, but the stripes pass “through” the shadow, as it were, and 
 emerge clean-cut and bright. The angles of extinction, with reference to the twinning 
 planes are, right 2°, left 9° 40’, and in another, right 2° 50’, left 8° 30’. Again, in another, 
 whose colours, in maximum illumination between crossed nicols, are, for one set of 
 lamelle, pale-yellow ; for the other, white. The angles are, right, 24°, and left, 5°. 
 Another gives right, 1° 10’, and left, 7°. 
 
 Orthoclase occurs in the usual Carlsbad twins, but not plentifully. All the 
 felspars exhibit more or less unduloes extinction. 
 
 The angles given above are taken from the central extinction as far as possible. 
 In one or two cases the stripes have violet centres and blue ends, with the quartz plate 
 and the analyser arranged for a violet field. Hornblende reedy (“schilfige’’) and 
 absorption feeble, much epidotized. The crystals have been seriously mutilated in the 
 process of grinding, the centres of nearly all being ground away, leaving microliths of 
 hornblende in a ragged state, arranged marginally around cavities originally occupied 
 by the mineral. 
 
 Magnetite and apatite, the former always and the latter occasionally, associated 
 with the hornblende. The apatite, however, is small and infrequent. One or two 
 hexagonal sections of apatite occur in the felspars. 
 
 Quartz in allotriomorphic grains, playing an insignificant part in the constitution 
 of the whole rock, pretty much of one size, Ol inch in diameter. The enclosures are 
 normal but large, in some cases fluid, in other cases glassy, and in afew gaseous. A few 
 translucent oxide of iron specks, only visible under the 4-inch objective. 
 
 No. 23. BovnpEer Creek, Srrent Grove, NEAR Mackay (QUEENSLAND). 
 A. G. Maitiand’s Collection. 
 
 Colour, red. Granular, allotriomorphic, holocrystalline; the contained minerals 
 include what looks like pink orthoclase, quartz, and a little hornblende. No mica 
 visible in hand specimen. 
 
712 
 
 * _RHYOLITES, Eve. 
 No. 1. FrErevusson Istayp, Dawson Srrarrs (NEw GuINEA). 
 Sir W. Macgregor’s Collection. Sp. Gr. 2°426. 
 
 Colour, black. Vitreous, containing numerous macroscopic quartz and sanidine 
 crystals. The crystals appear to be centres of cracking.* Fracture conchoidal. 
 
 Section.—Perfectly isotropic. Glassy base, with plentiful sprinkling of colour- 
 less rods, whose angle of extinction, being parallel with the principal axes of the nicols, 
 would indicate monoclinic felspar microliths. Some of the felspars are tabular, 
 measuring about ‘Ol inch in length and half or less in width, with very minute inclusions. 
 The rods are sometimes plates, looked at edgeways, but this is not always the case; 
 many undoubted rods occur whose arrangement discloses fluxion-structure. The 
 quartzes are large, measuring *06 inch to ‘1 inch in length, and filled with gas pores, all 
 fixed. The Drawing on Plate 66, fig. 1, exhibits one lenticular inclusion in the left- 
 hand corner of the quartz crystal, containing upwards of forty fixed gas pores. The 
 drawing also shows the two habits of the felspars, tabular and prismatic. The cracks 
 traverse the glassy base and the quartz crystal. Magnetite sparse, in well-formed 
 octahedra. Hornblende (?) green; in three instances with enclosed crystals of magnetite ; 
 a few pale-green hornblende (?) microliths visible under the + inch. The felspar laths 
 are mostly stepped, but the tabular felspars are perfectly he The higher powers 
 also show the existence of deposits along the cracks of the quartzes, ramifying, and spread 
 like the dentritic manganese deposits found in the joints of rocks. Very often these 
 cracks pass over the margin of the quartz crystal, penetrating into the contiguous glassy 
 base. Amongst the quartzes are many glass enclosures, whose contours are invariably 
 rounded, but never quite spherical, and the fixed gas bubble is generally at one end. 
 
 No. 16. Croncurry (QUEENSLAND). 
 R. L. Jack’s Collection. Sp. Gr. 2°297. 
 
 Colour, black. Vitreous. Opaque. 
 Section.—A perfect glass, a little traversed by cracks, in no particular direction. 
 A slab ‘01 inch thick is faintly illuminated between crossed nicols. 
 
 No. 3. Mironrert Rrver (QUEENSLAND). 
 R. L. Jack’s Collection. Sp. Gr. 2:72. 
 
 The rock is of a bluish-gray colour, in spheroidal lumps with conchoidal fracture. 
 
 Section.—Light coffee-coloured glass, perfectly isotropic. Spherical bodies occur 
 in the glass, one of which is shown in Plate 63, fig. 1. As there shown, some of these 
 bodies are certainly crystalline, and the crystals seem to have gathered round one point 
 asa centre, and grown outwards, absorbing the material for their growth from the glass. 
 The microlites near the centre seem to have had the best chance, and to have availed 
 themselves of it, for they are more distinctly crystalline than those more remote from 
 the centre, while the great opacity, and want, apparently, of crystalline structure in the 
 periphery, would suggest the rejection of the material that was of no use to the growth of the 
 crystals. The clear marginal zone round the globular bodies iz every case proves that they 
 grew by the abstraction of certain substances from the glassy base. (Vide Plate 63, fig. 
 1.4) ‘This is almost analogous to the assimilation of food-stuffs by plants and animals. 
 
 
 
 * These cracks must be produced by the unequal contraction, on cooling, of the quartz and the glass, 
 respectively. This suggests the question, what are the coefficients of expansion for quartz and glass ? 
 
 + The zone may be due to the heat developed in the crystallization, keeping the neighbouring glass 
 fluid, while the more remote was getting viscous. Thus no more supplies could be got for the growth of the 
 young crystals, except from the envelope immediately surrounding the sphere, which, being less viscous, was 
 more thoroughly drained of the material necessary for the crystal’s growth. 
 
713 
 
 No. 11. Mackay (QurEENSLAND). 
 A. G. Maitland’s Collection. 
 
 This rock is opaque, with a dirty reddish-yellow colour, and might belong to 
 either the obsidian or tachylite group. 
 
 Section—Only shows a few completely altered felspars and a dense opaque 
 yellow glassy base, which is isotropic on the feather-edge. Mr. P. F. Sellheim, Under 
 Secretary for Mines, kindly prepared this section for me. 
 
 No. 196. SwHerrretp (TAasMANTA). 
 
 R. L. Jack’s Collection. 
 
 Colour, black. Vitreous. Glass with clear little white crystals. This is by far 
 the most beautiful example of pitchstone I have yet seen. The crystals are olivine, and 
 they are mostly preserved in exquisitely regular forms in the glass; the faces 0 P (‘001) 
 are wanting. The section being a little thick and the glass very transparent, together 
 with their high angle of refraction, enables one to recognise in these crystals many of 
 the characteristic planes of the typical olivine crystal. In this rock, students of micro- 
 scopical crystallography have an opportunity of studying olivine in a perfect crystal 
 form. Under the 4-inch objective the olivines are seen to include glass with 
 fixed glass bubbles. The glassy base carries nothing else but opaque dusty matter in 
 spots, which is probably a darker glass nucleus fringed with dusty matter, in whose 
 neighbourhood gas bubbles are commonly found. The glass has bubbles at tolerably 
 regular intervals, and in one or two cases, bubbles are strung out in shapes or outlines, 
 
 The microlites are very small, and play no great part in the constitution of the 
 rock. They are tabular felspars, not unlike the New Guinea felspars in obsidian 
 described in the No. 1 of the Rhyolites. (Hor Drawing see Plate 64, fig. 2.) 
 
 No. 58. Mackay (QuEENsLAND): Setection No. 1642. 
 A. G. Maitland’s Collection. 
 
 Colour, light-brown. Vitreous. Fracture conchoidal, with strongly marked fissure 
 planes, not unlike slate in this respect, rendering it difficult to mount when the section 
 is removed from the grinding-slip. Under a lens, the rock is seen to carry numberless 
 whitish-yellow granules, which appear as yellowish patches on the plate. 
 
 Section.—Isotropic glassy base filled with most delicately matted microlites. In 
 the plate they appear too white; the real colour is a faint yellow. By reflected light 
 they have just the colour and sheen of the hair of a fair young child. They mark the 
 fluxion, which would otherwise be invisible. I cannot suggest a name for the yellow 
 patches, which are amorphous and well distributed, often enveloping the smaller 
 
 -felspars. 
 
 The two ovate bodies in the sanidine crystal are composed of the same substance, 
 and are between the two faces of the sanidine section, as verified by the micrometer- 
 screw. 
 
 The felspars are fairly fresh sanidines. The extinction-angle of the sanidine in 
 Plate 62, fig. 2, with reference to the crystal edge, is 24°, so that the section must be cut 
 slightly oblique to the clinopinakoid (010), since, were it exactly parallel, it would be 
 about 21°.* The rock is not quartzless, but only three small rounded quartzes occur in 
 a section ‘75 inch square. 
 
 * Rosenbusch. Physiography of the Rock-making Minerals, p. 281. 
 
714 
 
 No. 108. Neri Isre (New Guinea). 
 Sir W. Macgregor’s Collection. Sp. Gr. 2°407. 
 
 Section.—A. greyish glass filled with somewhat large felspar microlites, which 
 mark the fluxion-structure, as in Plate 61, and Plate 62, fig. 1. But even if the 
 microlites were wanting the fluxion would still be well marked by the dusty matter with 
 which the glass is charged. The felspars are very clear, almost limpid, and generally 
 of a tabular habit ; though some are prismatic, like the felspar, abutting on the olivine 
 crystal in the three figures on Plates 61 and 62. A felspar is shown thereon close to 
 the margin, which is slightly inclined to the plane of the section. It is one of the 
 tabular crystals, which, hading away from the olivine, has passed through the other 
 side, where it has been ground off with the slice. Sanidine, twinned on the Carlsbad 
 type, is pretty common, and exquisitely limpid. An olivine crystal is represented in 
 each drawing, abutting on a felspar, and the structure of the glassy base, shows 
 fluxion, as marked both by the microlites and the dusty matter. All three are magnified 
 forty-two diameters—(1) polarized between crossed nicols, (2) with polarizer only, and 
 (3) between parallel nicols respectively. 
 
 The roughness of the olivine is shown in Plate 61, fig. 1. The black crystals 
 on the margin and in the interior of the olivine are either magnetite or titanic iron, 
 more probably the latter. Under the }-inch objective the microliths are peculiarly 
 numerous. ‘They can be divided into two classes,—first, a large form of microlite, as a 
 rule measuring about ‘0005 x ‘004 inch, which are always stepped like the drawing given 
 in Rosenbusch*; and, second, hair-like microliths, which, however, are not trichites, 
 being transparent. The brownish-grey wave flowing over the felspar, shown in the 
 drawings, is very rich in these minute microliths. The feathered edge of glassy base on 
 the other felspar, just peeping out at the surface, on the right-hand side of Plate 61, 
 fig. 2 (also showing in Plate 62, fig 1), becomes very useful, as it enables us to get 
 a clear view of these small bodies without the image getting blurred by a background 
 composed of the same bodies, in different azimuths. In one of the clearest and most 
 limpid of the sanidines is a very curious growth of what I take to be a glass inclusion. 
 The growth starts from a poiut on the margin of the crystal, and branches out not 
 unlike a fern, but that the divergent branchlets are clubbed at the end, and are a pale 
 hyacinth colour. 7 
 
 TRACHYTE. 
 No, 24. GtapsTonge (QUEENSLAND). 
 R. L. Jack’s Collection, Sanidine Trachytes. Sp. Gr. 2°79. 
 
 Colour, dirty whitish-red; with somewhat large crystals of sanidine. Very 
 porous, with a few small cavities not unlike the smaller holes in a sponge. 
 
 Section. Ground-mass plagioclase, showing fluxion-structure; quartz in very 
 small allotriomorphic grains; sanidine, clear. One sanidine crystal is well marked 
 with curved markings as drawn by Rutley in the “ Study of Rocks”’ (p. 96, iii. edition) 
 and sometimes tabular, being parallel to J; at other times the sanidines are twinned 
 on the Carlsbad type. By reflected light one sees a very thorough sprinkling of the 
 whole slice with brownish-red ferritic matter, and a whitish-yellow substance, both 
 amorphous. Only the sanidines escape the peppering. 
 
 The slice being somewhat thick it is difficult to make out the glass that ought to 
 be present. The only glass observable is that lining the interior of cavities. 
 
 
 
 * Physiography of the Rock-making Minerals, 
 
715 
 
 MACKAY DISTRICT. 
 
 The following eleven rocks from the Mackay District, together with the very 
 excellent sections thereof, were kindly lent me by Mr. A. G. Maitland. They are, 
 without exception, the thinnest sections described in this Paper, having been sliced in 
 London by Mr. Cuttell, of Kentish Town. Drawings and sections showing the mode of 
 occurrence of the rocks in question, given in Mr. Maitland’s “ Report on the Geological 
 Features and Mineral Resources of the Mackay District,” * are reproduced in Plate 46, 
 figs. l and 2, of this Work. 
 
 (1) From a Gar on tHE Norru stpe or Mount Jukes. Sp. Gr. 2°490. 
 
 Colour, red, blotched with white specks. 
 
 Section.—Shows granulitie quartz, the grains about ‘01 inch; comparatively very 
 large orthoclase, as Carlsbad twins, the largest reaching ‘08 inch in length. These felspars 
 are dusty with ferrite, which gives the rock its colour. They areall kaolinized, and but 
 for the exceeding thinness of the section could not be identified. No plagioclase. A 
 few crystal wrecks with grains polarising in high colours on the margin of holes 
 originally occupied by a primary crystal. These grains have a clean bright aspect in 
 ordinary light and might be epidote or olivine. A good deal of opaque oxide of iron 
 incysts these brilliant specks. Under the +4-inch objective, the quartzes have a few 
 inclusions ; some may be glassy, others are certainly fluid with moving bubbles. (Vide 
 Mr. Maitland’s “ Report’’ and Section on Pl. 46, fig. 1.) 
 
 (2) Mount Martin, Jortmonr Creex. Sp. Gr. 2°570. 
 
 Colour, dirty brown. Fine-grained. The hand specimen looks like a felsite. 
 There are no porphyritic crystals. 
 
 Section.—Ground-mass a felt of microlites, without any glass, but between crossed 
 nicols feebly illuminated. Felspars much changed, packed with granules, which are the 
 only points of illumination throughout, the rest of the section being a dark-lavender 
 colour. The granules may be epidote. Orthoclase was a constituent mineral of the 
 rock, Magnetite (or titanic iron), with a little apatite, is present in small quantity, but 
 at fairly wide regular intervals. One hexagonal section of the latter measures about 
 ‘10 inch. 
 
 (3) Mount Manparana, “Tue Leap.” Sp. Gr. 2°498. 
 
 A white rock, speckled with small black grains and sanidine; highly porous 
 when applied to the tongue. 
 
 Section.—The ground-mass is made up of alittle granular quartz and numerous 
 felspar laths, and is holocrystalline. The macroscopic sanidine (Carlsbad twins) is 
 perfectly limpid and shows the faulting along the suture, the boundaries not participating 
 in the apparent movement, as pointed out by Rutley.t Under the }-inch objective, 
 the black specks turn out to be grains of deep-green mineral, with marked differences 
 of absorption when viewed with polarizing prism. With these specks, apatite, and 
 perhaps magnetite, is associated in fine grains. No fluxion-structure. In the felspars 
 of the ground-mass is one beautiful spherulite, the arms measuring nearly ‘03 inch, 
 but I cannot find another in the whole section, which is seven-eighths of an inch in 
 diameter. Mr. Maitland says :— 
 
 “One of the most conspicuous examples of the lavas is to be found at Mount 
 Mandarana, better known as the Black Gin’s Leap, close to the Bowen Road, about twelve 
 miles north-west of Mackay, where it forms a broad table-like mass, rising to a height 
 
 
 
 
 
 * Brisbane : by Authority : 1889. 
 + F, Rutley, The Study of Rocks, iii, Edition, page 44. 
 
716 
 
 of 650 feet, by corrected Ancroid, above the level of the Road. The rock of which the 
 Leap is made up is lithologically a trachyte, and may be generally described, when 
 examined with a lens or the unaided eye, as consisting of a light-coloured porous 
 matrix, in which crystals of sanidine and minute crystals of what appear to be horn- 
 blende are embedded. It is seen* to rest upon black shales, at a point in a 
 gully flowing from the north-west corner of the mountain three hundred feet above the 
 Road; at the junction of the two the shales for a few inches are slightly hardened. The 
 lower portion of the sheet is made up of rudely hexagonal curved columns, the outward 
 curvative being northwards. The structure of certain parts of this rock would seem to 
 imply that in reality it is a succession of lava-flows of variable thickness. The estimated 
 thickness of the sheet is not less than 350 feet.” 
 
 (4) SupaqurEous Turr, ALLIGATOR CREEK, Sarnt Hevens, Macway. Sp. Gr. 2°618. 
 
 This is a white porous rock, with reddish oxide of iron in strings and lenticular 
 veins. The section is cut transverse thereto. 
 
 Section.— All but quartzless, the grains being very few, small, and sparse, with 
 matted plagioclases in the ground-mass, the laths being clouded and ill-formed, measuring 
 under ‘01 inch in Jength. One or two much altered porphyritic felspars occur, with 
 traces of many lamelle. Dusty specks of a mineral polarising in higher colours occur 
 throughout the section, but they are too minute to resolve with the }-inch objective 
 The highest colour produced between crossed nicols in the ground-mass is slate-grey. 
 
 N.B.—Hydrochloric acid failed to produce effervescence except where the 
 section cut through an iron speck, when a very slight effervescence ensued, making one 
 suspect the presence of siderite. 
 
 (5) Mount JuKEs. 
 
 This rock is similar to (1) except that the colour is lighter, it being white. 
 The felspars glisten when the hand specimen is turned about in the light, owing to the 
 cleavage planes of the felspars catching and reflecting the rays. 
 
 Section.—By reflected light there is hardly any ferrite, and the orthoclase is less 
 -kaolinized. The quartzes limpid,as in (1). The rock is a perfect example of holocrys- 
 tallinity. There are but two constituent minerals—orthoclase in Carlsbad twins, dusty - 
 from kaolinization which is rudely paraliel to the cleavages, the latter making angles 
 with the plane of composition; and the quartzes, which have marked dihexahedral 
 inclusions, liquid, glassy, and gaseous. In some of the quartzes are moving bubbles. 
 Others with the dark margin, occur, denoting gaseous inclusions. The quartzes average 
 ‘Ol inch, the smallest being ‘002 inch, and the orthoclase sometimes ‘03 inch long by 
 ‘02 inch or less broad. Two or three jet-black lustrous grains, and a few longer or rod- 
 like of the same substance were not identified. Mr. Maitland says :— 
 
 * Another denuded wreck of an old volcano is to be found in Mount Jukes, 
 some 1,800 feet above sea level, and situated on the bank of Neilson’s Creek, and about 
 twenty miles distant from Mackay in a north-westerly direction. The mean specific . 
 gravity of the rock, from specimens in different parts of the mountain, was found to 
 be 2°55. Different parts of the mass present different characters, but generally two 
 varieties can be recognised— 
 
 (a) A coarse-grained rock in which a matrix can scarcely be said to exist; and 
 (4) A second in which erystals of sanidine and plagioclase are embedded in a 
 microcrystalline base, which, with the aid of a lens, is seen to be made 
 up of small crystals and crystalline grains of sanidine and hornblende (?). 
 
 * See Pl. 46, fig. 1. (A.W.C.) 
 
 
 
717 
 
 “The former variety, owing to its coarse grain, would be called a nevadite, whilst 
 the latter would be best described by the term sanidine-trachyte; both, however, are 
 merely varieties of one and the same rock. The rock is intrusive through the volcanic 
 series, and sends out here and there dykes of no great thickness, and of a somewhat 
 similar character to the rock forming the main mass. Hardly any apparent alteration has 
 taken place in the rocks through which the mass has burst.” 
 
 (6) Mounr Manparana. Sp. Gr, 2°46. 
 
 Colour white, with a tinge of blue. Microgranitic, holocrystalline. The whole 
 rock is made up mainly of ground-mass, there being very few porphyritic felspars. 
 
 Section.—Shows a little corroded mica, some minute specks of a mineral polar- 
 izing in high colours, with a greenish, sometimes colourless, tint. A very few 
 porphyritic felspars, probably oligoclase. A very regular seattering of grains of 
 hematite (or some translucent iron oxide) and a little interstitial glass spread over an 
 area of ‘05 inch, and not occurring anywhere else in the section. The mica shows complete 
 absorption for rays vibrating parallel to lamella when the section is normal thereto. 
 
 . 
 
 (8) Pinnacte, Hitisporovau. Sp. Gr. 2°49. 
 
 Colour, brownish-red. With marked fluxion-structure, porous and very fine- 
 grained. 
 
 Section.—Ground-mass highly felspathic, with well-marked spheroidal structure, 
 and but little quartz. A few specks of a mineral polarizing in high colours, and a few 
 water-clear sanidines. The angle of extinction right and left of the twinning line for 
 a twinned crystal is—right 9° 40’, left 19° 30’; this crystal measures ‘12 inch long by ‘04 
 inch broad, and is perfectly limpid. There are certain lines in the section, on either 
 side of which the microlites arrange themselves transversely. Whether this is a result 
 of fluxion is not certain. I have not seen fluxion-structure exemplified in this way 
 before. Mr. Maitland says :— ; 
 
 “ Another fragment of rock of this class is seen capping the Finlayson Hills, 
 22 miles north-west of Mackay, and about 14 miles from the sea-coast, where it forms 
 a sugarloaf-shaped peak, resting on granite, and rising to a height of about 100 feet 
 above the summit of the hills.* The rock has a matrix of a purple-grey hue, with well- 
 marked banded or ribboned structure, in which the lines of flow can often be seen to 
 bend round the larger sanidine crystals embedded in the base. As a whole, the rock 
 is much more compact than the Mandarana trachyte, and, like it, forms rudely 
 hexagonal columns.” : 
 
 (9) AtticaTor Creex, Saint HeLens. 
 
 Fine-grained brown rock. 
 
 Section.—By reflected light shows ferrite, white dusty specks, and occasionally 
 pyrites, without magnetite. Between crossed nicols there is no interstitial glass, and it 
 is difficult to say whether the much kaolinized felspar laths are embedded in a felsitic 
 mass or not, since although, as a whole, the laths are distinct, yet when a higher 
 power is used all definition disappears, the edges merging into a fine-grained granular 
 aggregate, sometimes polarizing brilliantly. The felspars are highly altered. Many of 
 them are filled with irregularly scattered grains of a very doubtful epidote. The rarer 
 sanidine is pellucid as usual. Calcite is occasionally seen in small grains in twinned 
 lamellez. The porphyritic crystals are represented by two or three wrecks of felspars, 
 
 
 
 
 
 * See Pl, 46, fig. 2. (A.W.C.) 
 
718 
 
 so changed as to be impossible to identify. Another remnant of what has been a large 
 prism, measuring ‘08 inch by ‘01 inch, is crossed by yellowish-red bars of a non-fibrous 
 but rather granular structure, feebly anisotropic. If this crystal could be restored and 
 identified, great light would be thrown on the whole matter of the origin and life-history 
 of this rock. Asa concluding observation, the proximity of calcite to the relics of this 
 crystal and its possible occlusion amongst the somewhat heterogeneous mass of secondary 
 mineral matter is to be noted. 
 
 (10) SrarortnH Hitis, West Srpr, Mackay. Sp. Gr. 2°48. 
 
 Colour, dirty grey, with a tinge of blue. Quartz is the only porphyritic mineral, 
 and is embedded in a fine-grained pasty-looking ground-mass. The whole rock is 
 sprinkled with fine blackish grains, The quartzes are very brilliant. 
 
 Section.—By reflected light, the ground-mass consists of kaolinized felspars, not 
 lath-like, but granular and pretty uniform. The black grains are innumerable, not 
 sharp, but irregular, and often surrounded by ferrite. Under the 3-inch objective the 
 fresh felspars are twinned, and might be orthoclase or sanidine. Owing to dusty matter 
 and kaolinization, it is difficult to identify these very minute felspars, particularly as 
 they are too small to be inspected under any lower power than the j-inch. There is no 
 interstitial glass or fluxion-structure. Quartz is the only porphyritic mineral, and is 
 rounded, showing, in two or three cases, the “ bays, inlets, and islands” peculiar to the 
 quartzes of the rhyolites and porphyrites. The quartzes carry liquid, gaseous, and 
 glassy inclusions. Mr. Maitland says :— 
 
 ‘Near the head of Niddoe’s Creek, one of the watercourses draining the 
 western side of that range of hills lying between the Main Range and the Coast, a 
 trachyte lava of a somewhat different character is seen dipping south-east at an angle of 12 
 degrees, and resting upon the sedimentary rocks of which this range is made up. 
 Lithologically the rock may be called a quartz-trachyte, and throughout it presents a 
 great uniformity in its physical characters ; it is made up of a light-grey, porous matrix, 
 in which quartz, sanidine, and small specks of what appear to be hornblende are 
 
 embedded.” 
 (11) Tue Pinnactr, Saint HELEns. 
 
 A nearly white rock, weathering red, very fine in grain, and without any 
 porphyritic minerals. 
 
 Section.—By reflected light. Fine-grained, without any porphyritic minerals, 
 with a few green and much corroded fragments and many minute specks of a reddish 
 semi-translucent hydrated oxide of iron. The base is microlitie, without any pasty 
 matter whatever, and is built up of orthoclase, plagioclase, and quartz, and the greenish 
 mineral may be mica very much corroded. Mr. Maitland says :— 
 
 “In the Parish of St. Helens, on the south bank of Alligator Creek, a lofty 
 ridge of mountains, the Pinnacles, which form a corry, encircling one of the branches 
 of this creek, a great thickness of lava occurs. The rocks are trachvtes of a brownish- 
 grey colour, and with which fine-grained trachyte tuffs are associated. The lava-sheets 
 have their steeper faces southwards, and appear to dip in a general northerly direction. 
 One of the sources from which some of these lavas and ashes have been ejected appears 
 to be Mount Barron, a steep, triple-peaked mountain, the highest summit of which is 
 about 2,000 feet above sea-level, and which is almost surrounded by the head-waters of 
 St. Helen’s Creek. (Section IV.) The rock of which this mass is made up is greyish- 
 white in colour, and somewhat porous, with a mean specific gravity, as determined by a 
 Walker’s Specific Gravity Balance, of 2°56. In the matrix, small crystals of sanidine 
 
719 
 
 and minute specks of a black mineral—probably hornblende—ean be recognised. 
 Throughout the whole mass, the rock retains very much the same character. The 
 mountain rises perpendicularly from the alluvial flat on the north bank of St. Helen’s 
 Creek, and in Barron Creek the mass is seen to be intrusive through an ‘ orthoclase 
 porphyry ’ upon which the sedimentary strata are seen torest. No perceptible amount 
 of alteration was detected in any of the sections in which its intrusive character was 
 observed.” 
 BASALT. 
 No, 2. Goopenoven Isuanp, Moressy Srrair (NEw Gurnea). 
 Sir W. Macgregor’s Collection. 
 
 Section.—Vesicular, with minute augite and felspar crystals visible to the naked 
 eye. Augite crystals are plentiful, with glassand magnetite inclusions. Mr. Maitland, 
 who has recently visited New Guinea, suggests that the augite may have to be referred 
 to enstatite ; in which case the rock would be classed among the andesites. The sanidine 
 crystals show growth by accretion in a very beautiful manner. The ground-mass is so 
 opaque that minute plagivclase crystals not thick enough to reach through and touch 
 each surface of the section do not appear by transmitted light at all, while by reflected 
 light a very large number of these minute pellucid crystals can be observed. 
 
 No. 173. Patm Ispuanp. 
 
 H. C. MecDonald’s Collection. Sp.Gr. 2°622. 
 
 Colour, speckled greenish-brown. The specks are yellowish. The rock has a 
 compact texture.* 
 
 Section.—This rock is so much decomposed that its section does not reveal very 
 much. Its constituent minerals are augite and felspar. Apatite (in considerable 
 quantities) and magnetite occur as accessory minerals. 
 
 The augite is much cleaved and shattered, the basal sections having very well- 
 marked cleavage, parallel to 1i0. 
 
 The felspars must once have been of great beauty (and their even size and 
 perfect twinning is still discernible). They are associated with a green mineral of 
 secondary origin, probably chlorite, plentiful, not regular in outline, not pleochroic, 
 differences of absorption nzJ, between crossed nicols appearing a speckled yellow-green ; 
 the specks do not extinguish uniformly. 
 
 No. 15. Normansy Reers, Cooktown (QUEENSLAND). 
 
 F. Bauer’s Collection. Sp. Gr. 2°808. 
 
 Colour, black, with reddish spots. Compact, slightly vitreous, fine-grained. 
 
 Section.—Ground-mass abundant, with idiomorphic hyalosiderite, or perhaps 
 fayalite, and plentiful hydrous oxide of iron, pseudomorphous after olivine. The latter 
 mineral exhibits all the stages of decomposition, some examples being quite fresh and 
 coffin-shaped, others having a deep-red margin and clear interior, others being only 
 specks, and others being without a trace of the original olivine. The olivines are the 
 only crystals of any size in the rock; they measure from ‘04 inch to ‘06 inch in length. 
 The rough look, owing to a high index of refraction, is marked. In one or two rare 
 cases the red envelope round an olivine is packed with magnetite. There are no 
 inclusions. The drawing on Plate XIX. of Rosenbusch’s “ Physiography of the Rock- 
 making Minerals” illustrates these olivines exactly. The ground-mass is peppered 
 
 
 
 * Mr. McDonald stated that this sample was taken from a dyke passing through a ‘‘ conglomerate ” 
 dipping towards the sea, 
 
720 
 
 with fine black lustrous grains, which are magnetite, as was found by testing a washed 
 sample of the pounded rock, and trying it with a magnetised sewing needle in a watch- 
 glass full of water under the microscope. There is a great deal of interstitial glass and 
 fine felspar microlites. Leucite occurs sparsely in small six and eight-sided sections. 
 Often in these crystals there is a central mass of inclusions consisting of magnetite and 
 microlithic felspars, leaving a glass-like hexagon or octagon perfectly free from any 
 inclusions, but with the angles generally rounded. But for this feature 1 might have 
 passed it over, but when once seen in the slice it becomes striking. The wearing of the 
 angles of leucite is noted by Teall.* No quartz or augite, and no fluxion-structure. 
 
 No. 75. Russrrn River (QUEENSLAND). 
 
 -R. L. Jack’s Collection. Sp. Gr. 2°864. 
 
 Colour, black. Compact. The fine crystals cause it to sparkle in the light. 
 The weathered surface is earthy, and coloured dirty yellow. Absorbent to the tongue. 
 
 Section.—Ground-mass glassy, matted with felspars, and perhaps very minute 
 augite (?) grains, sharp grains of magnetite and granular serpentine, &c. The section 
 is not thin enough for accuracy in these determinations. Olivine in fairly large crystals, 
 undergoing alteration to serpentine, is the only porphyritic constituent. The felspar 
 microlites in the ground-mass measure about ‘Ol inch by ‘O0Ol inch. Plate 65, fig. 1, 
 shows the olivines, the largest of which has a hole through it, which, of course, appears 
 black between the crossed nicols. The drawing shows the confused aspect of the base, 
 owing to the thickness of the section. Quartz absent. 
 
 No. 167. Surprise Creek, Herperton (QUEENSLAND). 
 
 R. L. Jack’s Collection. Sp. Gr. 2°64. 
 
 Colour, gray, with reddish-brown specks. Vesicular, with zeolites. 
 
 Section—Very rich in augite grains, which are about ‘0Ol inch in diameter, 
 plagioclase felspars and delicate microlitic needles permeating the felspars. No quartz, 
 and very little glass. The plagioclases are usually ‘02 inch long, and each is banded 
 three or four times, The only porphyritie crystals are much cracked. Augites invariably 
 enveloped in a red mineral of secondary origin. The augites carry minute enclosures 
 of glass and magnetite. Sometimes the secondary mineral has completely taken the 
 place of the augite. No orthoclase. Rich in magnetite, which occurs as sharp grains. 
 The rock would be better classed as anamesite than as basalt, all the constituent 
 minerals being of large size. 
 
 No. 169. ‘“Votcantc Hitt,’’ In Peterson’s Pocket, HerBERTON (QUEENSLAND). 
 
 R. L. Jack’s Collection. Sp. Gr. 2:291. 
 
 Colour, black. Vesicular, with grey streak. 
 
 Section.—Very vesicular, with large, fresh, much-cracked augite, sections of 
 which, parallel to clinopinakoid, have an angle of extinction of 25° 30’. Very fine- 
 grained ground-mass of microlithic felspars, and literally swarming with magnetite. 
 Magnetite and glass are the only enclosures in the augite. 
 
 
 
 
 
 * “British Petrography,” p. 366. 
 
721 
 
 No. 170. Avnerton’s Creex, Herperton (QUEENSLAND). 
 
 R. L. Jack’s Collection. 
 
 Colour, greyish-black. Very compact. 
 Section.—May be described in the same language as No. 167, except that the 
 minute felspar microliths are wanting, and the ground-mass is richer in augite granules. 
 
 No. 171. AtHERTON’s CREEK, HERBERTON UEENSLAND). 
 b>] 
 
 - R. L. Juck’s Collection. Sp. Gr. 2°738. 
 
 Colour, purplish-grey. Small vesicles. 
 
 Section.—The ground-mass is more glassy than in the preceding sample, No. 170, 
 and the augite is microgranulitic, with a little magnetite in the ground-mass. The 
 porphyritie augite is precisely similar in every respect to the last. The angle of 
 extinction on the clinopinakoid subtends an angle of 24° with the edge of the crystal. 
 
 The felspar microliths are long (about ‘92 inch), and seldom show more than 
 two stripes. They gracefully sweep past the obstructing augites, giving a fairly well- 
 marked fluxion-structure. It is by far the most interesting of the basalt collection, and 
 the section is peculiarly thin. 
 
 No. 251. Mirre Rock (New Gurnna). 
 
 Sir W. Macgregor’s Collection. 
 
 Colour.—A. dark greenish-black rock with yellow specks. 
 
 Section.—Ground-mass plentiful, consisting of a glass with innumerable felspar 
 microlites and sharp grains of magnetite. The felspars do not exceed ‘001 inch in 
 length, and the magnetite grains, which are wonderfully equal in size, measure ‘0002 
 inch in diameter. Fine black dusty matter makes the glass obscure, but under the 
 ¢-inch objective the constitution is resolved as given above. The porphyritic minerals 
 are plagioclase and augite, both very fresh, particularly the felspars. Sanidine in Baveno 
 twins with perfect zonal structure; also in Carlsbad twins. The best example of the 
 plagioclases several times twinned show angles of 26° and 24° 30' between the respective 
 axes of elasticity and the traces of the twinning plane JZ, so that the section must be 
 nearly normal to that plane. It is not certain whether this section cuts the basal 
 pinakoid or the clinopinakoid, but, whichever it may be, the formula of the mixture 
 cannot be less than Ab An.,* according to Rosenbusch’s table quoted in the granite 
 series. Zonal structure occurs in the plagioclases. 
 
 . The augite is in large crystals, averaging ‘06 inch, showing marked cleavage. 
 
 The angle between cleavage and an axis of elasticity is 28° 30’. The augites are but 
 little altered. In some cases serpentinization seems to have started. The inclusions 
 are glassy and gaseous. No moving bubbles. 
 
 - No. 214. Lotworrn Ron, rrom THE Foor of tHE Granite Ranar, Homestead, 
 Cape RrivER (QUEENSLAND). 
 
 W. H. Randy’ Collection. 
 
 A black, very fine-grained, compact rock. Carries no glass or pasty matter in 
 the ground-mass; might be a dolerite. The augite is microgranulitic. The felspars 
 are much striated. Compared with a section in a collection sold by R. Fuess, of Berlin, 
 
 
 
 
 
 * Where Ab represents albite and An anorthite. Vide Note on Rosenbusch’s Felspar Formule at 
 end of Chapter, 
 
 ax 
 
722 
 
 from Spiddal, it would be classed as a diabase, and, accepting Allport’s view that diabase 
 is really an altered condition of dolerite, it would be placed amongst the diabases, 
 following after the dolerites. (Professor Wadsworth places melaphyr, diabase, gabbro, 
 and many of the diorites under this head, so it may remain here.)* 
 
 Section.—Much augite in small grains, cracked ; little olivine, porphyritic augite ; 
 and exquisitely clear pellucid plagioclase felspars, showing several lameile. The angle 
 between the extinctions of the lamelle, right and left, is about 30°. 
 
 Nos. 51, 52, 53, 60, and 64. Tur BurpEKin River (QUEENSLAND). 
 A. W. Clarke’s Collection. 
 
 No. 266. Mount Razorpack, Upper BuRDEKIN (QUEENSLAND). 
 A. Gibb Maitland’s Collection. 
 
 No. 267. Mount Lane, Upper Burprkin (QUEENSLAND). 
 A. Gibb Maitland’s Collection. 
 Sp. Gr. of No. 266, 2°667; of No. 267, 2°477. 
 
 The first four rocks are from three well-known points on the Burdekin River— 
 viz., the “Top Rocks,” the “ Lower Rocks,” and the Crossing at Great Sandy Creek. 
 They are all vesicular black basalts. 
 
 The weathered rocks are often found with a white secretion in the vesicles, 
 probably zeolites.f 
 
 Section.—The ground-mass is made up of large plagioclase laths, ‘001 inch by 
 ‘02 inch, mostly stepped, and polarizing in high colours for felspars, and some doubtful 
 sanidine. The walls of the vesicles are lined with glass, in which occur afew very 
 minute specks, faintly luminous, but otherwise there is little glass and no fluxion- 
 structure. Magnetite in fine grains, plentiful. Augite in very small grains and 
 plentiful. The porphyritic minerals are olivine and augite. Along the cracks and 
 fissures of the former is a secretion of ferrite. The augite inclusions are glassy, with 
 fixed bubbles, and magnetite. 
 
 Unfortunately, the thickest section was that from which Plate 66, Fig. 2, was 
 drawn, so that the slice is too opaque, and in those crystals which do allow the light to 
 pass the colours are too high. However, in the drawing the olivines come out very well. 
 
 No. 266 differs from the preceding in the development of the transparent 
 hydrated oxide of iron which incysts some of the olivine, so that hyalosiderite or 
 fayalite must be reckoned amongst the varieties of olivine present in the rock. Certainly 
 a few sanidines exist, and a little glass eccurs. The rest of the rock may be described 
 in the terms of the preceding note on Nos. 51, 52, 58, 60, and 64. 
 
 In No. 267, the last of the Burdekin series of basalts, some beautiful prismatic 
 felspars oceur ‘05 inch by ‘002 inch, the angle of extinction with the edge of the pellucid 
 crystals being 0° or 8° and 4°. Otherwise the same description applies as to No. 266. 
 
 No. 72. Oxenpen, Mackay (QUEENSLAND). 
 A. Gibb Maitland’s Collection. Sp. Gr. 2°704. 
 A black, fine-grained, compact rock, with greyish-white streak. 
 Section.—Microgranitic, granulitic. Plentiful magnetite. Some highly-coloured 
 specks between crossed nicols, pointing to augite. No glass in the ground-mass, and 
 no porphyritic constituents whatever. 
 
 *M. EH. Wadsworth. Preliminary Description of the Peridotytes, Diabases, and Andesytes of 
 Minnesota, 1887. 
 + Black ants build their nests in the vesicular cavities of this basalt, 
 
723 
 No. 29. Near Baruurst (New Sour Watss). 
 
 The late Mr. C. 8. Wilkinson’s Collection. Sp. Gr. 2:993. 
 
 A black, fine-grained, compact rock, the faces of some of the constituents 
 glistening ; weathering yellowish-grey, and spotted; rarely with zeolites. 
 
 Section.—The ground-mass contains fine lath-like felspars, a little glass, por- 
 phyritic augite, and olivine with plentiful black grains of magnetite or titaniferous iron. 
 The felspars show fluxion-structure, arranging themselves in little streams dividing 
 before, and closing up after meeting an obstructing porphyritic erystal in the flow. The 
 felspars are about ‘01 inch in length. A greenish secondary mineral matter is often 
 secreted along the augite cracks. Magnetite frequent, enclosed in the augites. 
 
 No. 30. Baruurst (New Sourn WALEs). 
 
 The late Mr. C. 8. Wilkinson’s Collection. Sp. Gr. 2°951. 
 
 Black, compact, with occasional spots of zeolites. Weathering to a yellow 
 ochreous colour. 
 
 Section. —The ground-mass contains fine lath-like felspars, with very minute grains 
 polarizing in high colours, probably augite, and very little glass. The porphyritic augites 
 are asa rule fresh, though in some cases tne secretion of greenish matter is to be observed 
 along the very irregular cracks. Some water-clear plagioclase felspars occur with a very 
 wide angle of extinction between broad and handsome lamelle, polarizing in a low colour. 
 The highest angle of extinction observed was 63° 30’, and the lowest 32°. The fluxion- 
 structure is even more prettily marked than in No. 29. One of the augites shows 
 distinctly cross cleavages (which, however, are not very regular) parallel to the face 
 oo P. Another augite shows twinning in an interesting manner, there being three lines 
 along the suture, as in the section of the Gympie augite illustrated on Plate 65, Fig. 2. 
 The whole section swarms with magnetite. 
 
 No. 31. Mount Sassarras (New Soutn Wates). Intruding through the Hawkesbury 
 Formation. 
 
 The late Mr. C. S. Wilkinson’s Collection. Sp. Gr. 2°816. 
 
 Greyish-black. Crystals quite visible owing to reflection. No zeolitic matter. 
 
 Section.—The ground-mass has very little glass, and is much charged with 
 a dirty brownish-green opaque matter. Magnetite and plagioclase felspars. On the 
 margin of one of the olivines is a stellate group of secondary secretions, which polarize 
 in the aggregate, one portion certainly spherulitic, Augite and olivine oceur por- 
 phyritically, the latter a pinkish-brown, and dark, polarizing in high colours, and much 
 pierced and riddled by the felspars. Crossing the junctions are fine needles, probably of 
 apatite. The latter also abounds throughout the ground-mass. Magnetite is plentiful, 
 as is probably also titanic iron. 
 
 A rather large augite crystal is traversed by cracks, along which there are 
 secondary deposits. Their pleochroism is exceedingly remarkable, in some cases sky 
 blue, yellow; and green, very distinct. The periphery of this large crystal is marked by 
 a dark-brown zone, and extending radially into the contiguous ground-mass is a fine, 
 delicate, semi-translucent, aggregately-polarizing fringe. Arranged in the same way 
 under the 4-inch objective, this fringe is seen to be composed of fine microliths, clear, 
 and rather short, very much crowded together, owing to which there is no extinction in 
 any azimuth. The augite is rich in gaseous pores, 
 
724: 
 
 No. 309. Vicoror1a: OME. 
 
 P. Platt’s Collection. Sp. Gr. 2°71. 
 
 Greyish-black. Compact. 
 
 Section.—A compact basalt, with lath-like felspars, doubtful olivine, and grains 
 of magnetite. A yellow isotropic glass occurs amongst the crystals. Fluxion-structure. 
 A yellow envelope, precisely similar to the above, encloses an augite crystal, which has 
 symptoms of spherulitic structure. 
 
 No. 310. Batrtarat (Victoria). 
 
 P. Platt’s Collection. Sp. Gr. 2°54. 
 Greyish-black. Compact basalt from core of diamond drill. 
 Section.—The texture is nearly the same as the above (No. 309), but the slice 
 is too thick for much keen observation. The yellow isotropic mineral is rare. 
 
 DOLERITES. 
 
 No. 47. Govan (New Soutn WALtgss). 
 The late Mr. C. 8. Wilkiuson’s Collection. Sp. Gr. 2°964. 
 
 Black. This is a compact basalt, speckled with white crystals. 
 
 Section. —The rock is granular, idiomorphie and holoerystalline. The plagioclase 
 felspars are often ‘03 inch by ‘002 inch, and the majority are a pale-lavender, with very 
 small angles of extinction between the sets of lamelle, which latter are repeated many 
 times in all of the crystals. Other plagioclases have high angles of extinction, and 
 polarize in higher colours—i.e., in light yellow and orange. The latter often exhibit 
 undulose polarization. 
 
 Olivine somewhat large and fresh. Augite granular, with granulitic structure 
 as defined in Professor Hutton’s Paper before alluded to. Magnetite sparse. Very 
 little apatite, and no interstitial glass. 
 
 No. 35. Wottoncone (New Sour WaAtss). 
 The late Mr. C. S. Wilkinson’s Collection. Sp. Gr. 2°778. 
 
 Colour, brownish black. 
 
 Section.—Semi-crystalline, the lath-shaped felspars being separated from each 
 other by felsitic matter. Magnetite and perhaps titaniferous iron most abundant. 
 Augitic matter in very small granules, and not abundant. There is no interstitial glass. 
 
 Nos. 18 ann 19. Surniuemm Sinver Mines (QUEENSLAND). 
 (No. 18 is from the surface, and No. 19 from 30 feet depth.) 
 
 R. L. Jack’s Collection. Sp. Gr. of No. 18, 2°854. 
 
 Colour, dark-grey, speckled with what looks like hornblende. 
 
 Section.—Both show similar contained minerals, with the exception of hydrated 
 iron oxides, which are abundant in No.18. The minerals are so altered that even on the 
 thinnest feather-edge there is nothing very clear or worthy of description. The rock is 
 mainly composed of lath-shaped felspars, some being tabular and frame-shaped. Needles 
 of apatite are plentiful, in fact I have never seen a rock-section so crowded with this 
 mineral. Ina single group of quartz crystals, there is a continuous band ‘22 inch long, 
 containing apatites, cut parallel and at right-angies too P. They are of various sizes, 
 ranging from the finest hair up to prisms ‘001 inch in diameter, and from ‘02 inch to 
 ‘03 inch in length, 
 
725 
 
 Magnetite completes the list of constituent minerals that can be identified. 
 The felspars are filled with a granular deposit, some grains of which polarize in high 
 colours, and may be epidote. Some rounded grains also are to be observed in the 
 felspars, which polarize in high colours and might be put down either as olivine or 
 augite, more probably the latter. 
 
 No. 71. Tue Lear, Mackay (QUEENSLAND). 
 
 A. Gibb Maitland’s Collection. 
 
 Section.—This is another rock whose mineral contents are wholly changed and 
 altered. The ground-mass has been micro-granulitic and holocrystalline, with idio- 
 morphic crystals of lath-shaped felspars. There are a few fairly large porphyritic 
 orthoclase crystals, some of which are ‘06 inch long, twinned on the Carlsbad type, and 
 a few triclinic felspars. The plagioclase felspars show marked fluxion-structure in the 
 
 rock, 
 Quartz very sparse, in grains with rounded edges, carrying inclusions, some of 
 
 which have fixed bubbles, and others are glassy. No moving bubbles. 
 A little pyrites and magnetite make up the rest of the rock. 
 
 No. 21. Mount Kincuant, Mackay (QUEENSLAND). 
 
 A. Gibb Maitland’s Collection. Sp. Gr. 2°816. 
 
 Colour, grey, speckled with white felspars. 
 
 Section.—One turns with relief from examining the ill-defined wrecks of 
 crystals in the last three rocks to this; with its fresh, clean-cut, many-striped felspars. 
 Epidote is in fan-shaped groups. Magnetite, much of it sharp; and apatite in fine 
 needles. 
 
 The texture is not holocrystalline, there being a pasty mass of felsitic matter 
 separating what would otherwise be contiguous crystals. Felspars striated many times, 
 often over five, and once over forty times. The angle between the axes of extinction 
 for each set of lamelle in the largest felspar is 27°20’, and it measures ‘161 inch by 
 ‘Ol inch. Many of the tabular felspars are built up zonally. 
 
 The epidote is sometimes in rods, decidedly pleochroic ; at other times it is in 
 fan-shaped groups, merely showing differences of absorption on rotating the stage 
 over the polarizer. 
 
 The magnetite is sometimes in sharp, clean octahedra, and sometimes rounded, 
 
 The apatite, which is sparse, is in fine needles. 
 
 ; DIORITES. 
 No. 246. Sweprennore Reer, Coarrers Towers (QUEENSLAND). 
 
 The Hon. H. Mosman’s Collection. Sp. Gr. 2°866. 
 
 Colour, greenish-black. Speckled. Perfectly clear, fresh. Microgranular, 
 holocrystalline. 
 
 Section.—The felspars, although minute, are very perfect, often twinned several 
 times. Angles of extinction between parallel lamelle vary from 11° to 60°. The 
 perfect rulings of these felspars are very beautiful when viewed between crossed 
 nicols. Hornblende in about equal proportion to the felspars, showing marked 
 absorption and perfect intersecting cleavages when cut parallel to basal pinakoid, often 
 punctured by apatite prisms. Magnetite and possible ilmenite common. One or two 
 specks of titanite, being bright yellow with a high index of refraction. Perfectly 
 colourless transparent microliths commonly occur in the felspars. Very little accessory 
 quartz. 
 
726 
 
 No.13. Day Dawn P.C., Coarturs TowErs (QUEENSLAND). 
 A. W. Clarke’s Collection. Sp. Gr. 2°949., 
 This sample of rock comes from the No. 10 level, and is almost black in colour, 
 very fine in grain. 
 Section.—Hornblende is the prevailing mineral. With ordinary light, itis in very 
 slender long needles which are felted together. The felspars are plagioclase, and not 
 clear as in the last example of diorite. No quartz, and but little magnetite. 
 
 No. 17. Quarry Reserve, Mount Atma, Coarters TowErs (QUEENSLAND). 
 A. W. Clarke’s Collection. Sp. Gr. 3:057. 
 Colour as in No. 13. 
 This is a very similar diorite to No. 13, being of interest only because the 
 
 diorite No. 13 is from a depth of about seven hundred feet, while this is a surface rock 
 distant about one mile from the mine. 
 
 PORPHYRITES. 
 Nos. 129 ro 151. Croypnow (QUEENSLAND). 
 Sp. Gr.: Mean, 2°542; Extremes, 2°396 and 2°640. 
 
 In the following description a good deal of ground is covered ; the notes being 
 culled from some twenty-three rock samples collected by Mr. Jack. At one end of the 
 series, the rock is jet-black, very compact, with conchoidal fracture, and studded with 
 quartz whose surface of fracture is coincident with that of its matrix. At the other end 
 of the series, the rock is milk-white with identically similar quartz. The rock occasionally 
 shows blebs of graphite, and about the middle of the series the hand specimens appear 
 banded with different coloured varieties of the same rock. The larger quartz grains 
 cause waves in the banding, just as in sections of the rhyolites. 
 
 The following notes on the microscopic sections do not throw much light on 
 these rocks, and the whole matter is in the hands of the Geological Survey Department, 
 but they form an item of information which may not be devoid of interest :— 
 
 Ground-mass under the 2-inch objective shows no interstitial glass, and polarizes in 
 a hazy way, but every illuminated speck suffers extinction in the course of revolution of 
 the stage. Perfectly opaque, amorphous patches of a white substance (not unlike kaolin) 
 are distributed over the slice. By reflected light these patches are seen to aggregate 
 together. Part of the ground-mass is coarser in its crystalline structure than are other 
 portions, and the quartzes are all more or less penetrated by it in the shape of bays, 
 inlets, and islands. ‘The isolated ground-mass in the quartzes is due probably to the 
 transverse sectioning of a penetrant tongue. There are the wrecks of orthoclase 
 erystals. The ground-inass has so penetrated and become part and parcel of the original 
 crystals that it is difficult to speak with certainty as to whether they were sanidine. 
 
 In the quartzes are numerous glass-inclusions with fixed, and some few moving 
 bubbles. There is a patch of faintly green granular particles mixed with the ground- 
 mass. The green grains are very faintly dichroic (famt green to pale faint yellowish- 
 green). The quartzes are mostly rounded cn their edges and angles. 
 
 In other sections the pale-green granular Aceh are seen aggregated together 
 in what appears like the wreck of a crystal. These flecks are faintly dichroic, and in 
 one aggregate there is possibly apatite, but it is uncertain. The very small green 
 grains are sometimes numerous, and, under the 4-inch objective, allotriomorphic. They 
 are not dichroic. 
 
 Some patches of undoubted hornblende occur, which, though not very fibrous, 
 are too much changed to allow me to speak certainly on this point. Black, opaque 
 
 h_—e—=__*—_mee 
 
127 
 
 masses appear in juxtaposition with the hornblende. They are also amorphous, and 
 may be graphite. Occasionally brown hornblende occurs, which, as usual, is very 
 strongly dichroic. Epidote occurs amongst the altered hornblende. It is white, and 
 polarizes of course brilliantly. Some few yellow varieties occur; and in one of the 
 white epidote masses, a few microliths, that favour the monoclinic felspar variety, occur, 
 
 shaped thus :— 
 
 In the reddish varieties of the porphyry, ferrite is plentiful. 
 
 Mr. Jack, in a letter to me, dated Croydon, 4th December, 1889, states that this 
 rock “forms the hills lying side by side with the syenite forming the flats, and in which 
 the reefs of Croydon proper lie. The junction runs N.W. to S.E., just a few chains 
 off the Queen line of reef for two or three miles, and so straight as to suggest a 
 fault.” 
 
 
 
 
 
 
 
 
 
 
 
 x 
 Vg Kew Ka he 
 x 1S CER OL 0) ee 
 
 PP ts ee Oe . 
 OPP ON ALA ea ae 
 Ce caus Ce eer CK Me Ae ee Hy. ie 
 te On ie RE ee ores SS ES eh Pr oe 
 KNEE RE CI RIC TRS Sr Rie 2e 
 
 
 
 x 
 x 
 
 
 
 
 
 
 
 
 
 
 
 
 “T have never seen the syenite intruding through the quartz porphyry, or vice 
 versd. Then again the quartz porphyry shows fluxion-structure in a manner 
 suggesting a true igneous rock. Further, the quartz porphyry at times weathers so as 
 to show apparently purely siliceous, rounded enclosures, suggestive of an altered 
 conglomerate. The quartz porphyry (as well as the syenite) is full of little nests of 
 graphite, also suggestive, I think, of metamorphism.” 
 
 Nos. 79 anp 80. Great NortHern Tin Mine, HERBERTON (QUEENSLAND). 
 
 No. 79 is from three hundred feet below the surface. It is a grey elvan, with 
 glassy spots of quartz, and occurs as a dyke in granite. 
 
 Section.— Elvan with felsitic base. This is really a quartz-porphyry: a 
 microcrystalline granite base, with porphyritic quartz. The felsitic matter, under the 
 highest powers, carries light-green specks, quartz, and felspar, but there is no absolute 
 certainty about these minerals except that the green specks show faint absorption 
 when the stage is rotated over the polarizing nicol without the analyser. The ground- 
 mass is dusty, and carries rare pyrites. The quartzes show corrosion and rounded 
 contours, with the usual bays, inlets, and islands filled up with the ground-mass. 
 These quartzes are from 0:2 inch to 0'4 inch, and one is 0°8 inch in diameter. The 
 specific gravity of the rock is 2°603. 
 
 No. 80 is from the same dyke cropping out at the surface, and is precisely the 
 same as No. 79, but for the reddish colour due to weathering. The specific gravity of 
 the rock is 2'559. 
 
 Section.—Felsitic matter much more opaque and dusty, and quite impossible to 
 resolve. Porphyritic quartz, whose edges and angles are much less rounded and corroded 
 than is the case with No. 79. They measure from 0°3 inch to 05 inch. The felspars 
 are represented by one much altered twinned plagioclase, whose angle of extinction, 
 between the two sets of lamelle, is only 1° or 2°. It is 100 inch long, is often twinned, 
 
728 
 
 and the whole space occupied by the late crystal is now filled by little specks of a 
 highly-coloured mineral (between crossed nicols) in addition to dusty kaolin. The 
 specks may be mica or epidote. 
 
 No. 95. AtuErtTon’s CREEK, Mackay (QUEENSLAND). 
 
 A. Gibb Maitland’s Collection. Sp. Gr. 2°66. 
 Colour grey, with small black specks and small flesh-coloured felspars. 
 Section.—Felspathic spherulites, contiguous, without interstitial paste, but some- 
 times with intervening microgranulitie quartz. Dusty porphyritic felspars, packed with 
 specks showing high colours between crossed nicols. These specks are distributed in a 
 
 base whose definition is hazy and suffers partial extinction on rotation of the stage, . 
 
 while some of the specks remain illuminated in all azimuths. The felspars measure 
 from ‘O01 inch to ‘02 inch, and some show faint twinning bands. Occasional porphyritic 
 quartz, very much corroded. Some ill-defined chlorite and very sparse apatite. 
 
 No. 5. Gympre (QUEENSLAND). 
 
 R. L. Jack’s Collection, “‘ Greenstone.” Sp. Gr. 2°49. 
 
 Colour green, with white streak, and speckled with slightly deeper green spots. 
 
 Section.—It is not easy to describe this rock. It is highly metamorphosed, 
 no component mineral being now in its pristine state, with the exception of a few small 
 augities, whose sections are parallel with the basal pinakoid, and show cleavage parallel 
 to prisin-faces (parallel to 110). They are the only shining lights of the section, except 
 doubtful epidote grains. There is a pasty ground-mass filled with felspar microliths. 
 The porphyritic felspars are impossible to name: they merely present confused 
 kaolinized patches with opaque specks, which, by reflected light, are found to be milk- 
 white. 
 
 The hornblende or augite cavities, on the other hand, show light, bright-green, 
 very translucent patches, polarizing in very low colours, almost requiring the quartz 
 plate to discern, in many cases associated with a little apatite. This light-green mineral 
 of secondary origin might be chlorite, or,as Mr. Jack suggested, viridite. In one or 
 two cases there is a lattice structure, polarizing in vague blue slate colours, but it is 
 ill-defined. 
 
 At first sight the section looks uncommonly like a porphyry. The lattice 
 structure may possibly be serpentinous, and derived from the pre-existent augite. 
 
 New Sourn Waters. Marked “ Intrusive Dyke-stone from the Peak.” Plate 60. 
 The late Mr. C. 8. Wilkinson’s Collection. 
 
 Colour, dirty brownish-red, coloured with green spots. 
 
 Section.—The chief interest of this rock lies in the abnormal development of 
 epidote, which, in fan-shaped groups and green laths, fills the space probably at first 
 occupied by augite. The colours between crossed nicols are very high. The index of 
 refraction is high, and the pleochroism is fairly marked, so that there is little doubt 
 about the presence of epidote ; but there is an uncertainty with regard to the percentage 
 of these epidotes, for in no single instance has the change been incomplete. ‘The shape 
 
 and angle of the prisms suggest augite. Originally the crystals were perfect in shape, — 
 
 since the outlines are even now clear and sharp. The prism-angles I made out to be 
 about 88°. There is abundant apatite, and there are also transparent red grains, 
 while ferritic matter is developed with and alongside of the epidote. The rest of the 
 section calls for little description, the ground-mass being microfelsitic. The porphyritic 
 
 —— 
 
 ace 
 
729 
 
 felspars are large, measuring from ‘05 to ‘linch long. The angle between the axes of 
 extinction for the two sets of twinned lamelle in the largest felspar shown in Plate 60 
 is 14°, 
 No. 177. Mount Biscnorr (TasMantia). 
 R. L. Jack’s Collection: Sp. Gr. 2°783. 
 
 Colour, a dirty-white rock, with a few dark specks. 
 
 Section.—Ground-mass microgranulitic. Quartz and felspars with prophyritic 
 quartzes, not very much corroded. Felspar forms filled up with felsitic matter and a 
 radially-arranged mineral, highly coloured between crossed nicols. The quartzes carry 
 inclusions with moving bubbles, often dihexahedral. Dirty greenish-black, semi- 
 translucent grains are pretty evenly distributed over the section. They polarize feebly 
 under the 4-inch objective. 
 
 Nore.—The following is an extract from the ‘‘ Physiography of the Rock-making Minerals” (p. 292), 
 explanatory of Rosenbusch’s Formule for Plagioclase Felspars, referred to in the foregoing notes (pp. 703 
 and 721). 
 
 ae chemical composition of the theoretical albite is Na,O, Al,O;, 6 SiO,=Na,, Aly, Sig, 
 O|,=Ab; that of anorthite, 2 CaO, 2 Al,O,, 4 8i0,=Ca,Al.,, Al,, Siz, O,,=An. All other lime- 
 soda felspars, then, are isomorphous mixtures of albite and anorthite=Abn, Anm. Of the many possible 
 mixtures, certain ones occur more frequently, and have received particular names. If these be enlarged by 
 
 the addition of those compounds closely connected with them, then, following Tschermak, the lime-soda 
 felspars or plagioclases may be brought into the following table :— 
 
 Albite series embraces the compounds _... .. «b,, Ano—Ab,, Any. 
 Oligoclase series * fe .. Ab,, An,—Ab., An,. 
 Andesine series ss ae .. Ab,, An,—Ab,, Anj. 
 Labradorite series a ee .. Ab,, Anj—Ab,, An,. 
 Bytownite series er as .. Ab,, An,—Ab,, Ang. 
 Anorthite series 3 Pe Ab,, An,—Ab,, An,.” 
 
 SUMMARY. 
 
 The foregoing notes throw no new light on the science of petrography. Indeed, 
 one is struck with the microscopical similarity of the crystalline rocks of Australia, 
 America, and Europe. 
 
 In many of the granites almost the same language can be used in describing the 
 structure and constituting minerals of the innumerable varieties of the group as is 
 employed by authorities like Rosenbusch, Rutley, Teall, Zirkel, and others. 
 
 This is no deterrent, however, to the student, because the very sameness of our 
 crystalline rocks with those of other parts of the world proves the uniformity of those 
 chemical and physical forces which operated so powerfully in their formation and 
 subsequent mutations. 
 
 In all branches of science the recording of facts is the preliminary work. The 
 arrangement and classification of these facts generally falls to the lot of a distinctly 
 different type of worker. I have endeavoured to contribute something to the pre- 
 liminary work. 
 
 The rocks described are divided into six groups, viz.:—Granites, Rhyolites, 
 Basalts, Dolerites, Diorites, and Porphyrites. 
 
 GRANITES. 
 
 The quartzes of this group do not radically differ from those of the ordinary typical 
 granites. Allusion may be made to the long, brilliant, colourless needles, particularly 
 noticeable in the Croydon granite. They are not plentiful, possibly they are rutile, but 
 might be apatite, though from their solitary habit I think the first more likely, as 
 suggested by Teall in describing the Scotch granites. Many quartzes in this group 
 carry such inclosures. 
 
 The hornblendes, both green and brown, are sometimes fringed with epidote. 
 Occasionally a bluish-green envelope surrounds a deeper green or brown variety. It is 
 
730 
 
 to be noted that epidote generally secretes itself on the felspar frontier rather than the 
 quartz; that is to say, a hornblende bounded by quartz and felspar prefers to secrete 
 the secondary mineral on the felspar boundary. 
 
 The micas, black and white, do not commonly exhibit that piercing with apatite 
 which is frequent in the micas of typical German granites. 
 
 The felspars are, as a rule, exquisitely banded, and sometimes perfectly limpid. 
 The fibrous structure in some of the felspars is to be noted, but not confounded with 
 twinning. 
 
 Some of the orthoclases are very highly kaolinized, as is usual. Microcline 
 intergrows with orthoclase, particularly in the Etheridge samples. 
 
 Undulose extinction is most marked in the Charters Towers granites ; and with 
 regard to this matter I may quote Teall’s “ British Petrography” (page 33) :—“ Zonal 
 structure unquestionably indicates changes in the environment of the crystal during 
 the period of growth. The separation of crystals in a magma must necessarily produce 
 a change in the composition of the part which remains liquid; and this cause alone may 
 explain such cases as those observed by Hépfner and Becke. Changes from green to 
 brown and vice versé observed in certain hornblendes can probably be explained on the 
 assumption that the growing crystals were alternately subjected to oxidising and 
 reducing agencies. Until we are more fully informed as to the chemical and physical 
 changes which occur during the period of erystal-building in igneous magmas, and the 
 effects of such changes on the growing crystals, we cannot, however, hope to render 
 a complete account of the various structures observed in the crystalline constituents of 
 igneous rocks.” 
 
 The accessory minerals are not so minutely described as is usual in this branch 
 of science. I have not recognised any of the cubes, supposed to be salt cubes, in the 
 quartz inclusions, neither have I noted any microscopic zireons, which are generally 
 found in some samples of granite; but, as the prepared sections are to be handed over 
 to the Geological Survey Department, it will be possible in the future for others to 
 search more diligently, and with better instruments than are at my disposal. 
 
 Apatite, as an accessory mineral, nearly always is found in the vicinity of 
 magnetite. Particularly is this so in the Charters Towers samples of granite. 
 
 The tourmaline granite of Cooktown is interesting from the fact that the Cornish 
 tourmaline granite may be described in nearly the same language, and both are tin- 
 bearing districts. 
 
 Teall says :—“ The amount of tourmaline increases towards the margins of the 
 granitic masses. The increase in the amount of tourmaline is accompanied by the 
 disappearance of mica, and finally of felspar, the ultimate result being a rock composed 
 of tourmaline and quartz (schorl rock).” But whether this holds in the Cooktown 
 district is unknown to the Author. 
 
 The garnetiferous granite of the Cape River Gold Field bears out Zirkel’s. 
 observation that the American garnet-bearing granites do not carry the mineral in 
 microscopic size, all the garnets being macroscopic.* 
 
 ; RHYOLITES. 
 
 These rocks exhibit fluxion-structure. Zirkel describes them as follows +:—‘ In 
 the glassy and half-glassy rocks, it is a widely-spread phenomenon for the colourless 
 green and black, needle-formed, microscopical elements to be grouped together into 
 strings, bands, and flocks. There are bodies among them which have the appearance of 
 
 
 
 
 
 * Microscopical Petrography.” 
 + Loc. ctt., p. 4 
 
731 
 
 undulated and bent streams, damming up before a larger crystal, and flowing around it 
 to unite on the other side (giving the crystal something the appearance of an eye), 
 often also really scattered and dissipated by one of them. These appearances 
 evidently indicate that the fluctuations happened iu the stiffening glass magma, after 
 the microlites or little needle-formed crystals had been solidified. Analogous pheno- 
 mena of motion, fluctuation or fluidal structure, invisible to the naked eye in the hand 
 specimens, are very often observed in the thin sections of partly ‘or almost wholly 
 erystalline massive rocks, such as basalts, trachytes, phonolites, melaphyres, and green- 
 stones. The smallest ledge-formed sections of orthoclastie or plagioclastic felspars, 
 prisms of hornblende or augite, microlites of a variety of kinds; in short, all the 
 microscopical bodies possessing a longitudinal axis, are locally grouped parallel to one 
 another, and form undulating streams which diverge in the form of fans or ice-flowers. 
 Where larger crystals lie in the paths of these crowded bands, the little needle-formed 
 erystals encircle them on all sides with a tangential arrangement, are turned aside into 
 different paths, or come to an abrupt end before them, as if by a shock, the microlites 
 being thrown asunder in all directions. Observations of these phenomena of fluidal 
 microstructure are best made between crossed nicols, for the single crystals are then 
 coloured, and exhibit their characteristic direction much better than in ordinary light. 
 A low magnifying power best enables one to overlook at once a larger portion of the 
 then section, and thereby to follow the lines of fluctuation. The shape of the little 
 erystals is not without importance in the distinct observation of the form of the fluctua- 
 tions. If they are needle-like or ledge-formed, even feeble movements of the mass will 
 be unmistakably expressed ; if, on the contrary, they are of a roundish, granular form, 
 it often happens that strong fluctuations which have taken place fail to leave a trace of 
 their action. In some rocks, especially the rhyolites, this wavy structure is produced 
 by small dark grains grouped into lines and bands. These lines of grains undulate in a 
 most remarkable manner, so that the figures of their curvature resemble marbled paper. 
 There are also curled and twisted stripes of felsitic material, aiffering in colour and 
 behaviour, which render the waving motion evident. 
 
 “ Three important points present themselves upon which light is thrown by this 
 remarkable microstructure, connected with the fluctuations of the solidifying mass. It 
 proves that the rock was at one time a magma, in a plastic state, and that, after larger 
 crystals had been secreted, a shifting and displacement of the small microlites happened. 
 Soon afterward the mass seems to have been so suddeniy solidified that the streams 
 became fixed, and their fluctuation preserved for our observation. And, from these 
 facts, the conclusion follows that the large and small crystals were not formed exactly 
 where we perceive them, but that they have been thrown into their present place by the 
 purely mechanical action of the surrounding plastic mass. It is worth mentioning that 
 those rocks whose microfluidal structure is particularly distinct, are generally propor- 
 tionately rich in broken crystals, shivered into detatched, sharply angular fragments. 
 And, lastly, this structure proves that the smallest crystals of the rock have not altered 
 their mutual grouping and form, which date back to their solidification; and that, 
 although secondary decompositions may have occurred in the lapse of time, these 
 metamorphic influences have by no means been sufficient to obliterate the original 
 characteristic structure.” 
 
 The word “‘rhyolite’’ is compounded from fvag (a lava stream), and Aios (a stone), 
 and was first introduced by Richthofen in 1860. 
 
 I was somewhat exercised as to the inclusion of the quartz-trachytes of Mackay 
 in the group, but Rutley says * :—‘‘ Some petrologists include obsidian, pitchstone, 
 
 * «The Study of Rocks,” p. 177, 
 
732 
 
 perlite, pumice, and certain quartziferous trachytic lavas, under the terms rhyolite and 
 liparite. The student should therefore bear in mind the fact that the separation of 
 the vitreous from the erystalline rocks refers merely to physical differences which the 
 members of these two sub-classes respectively present, and does not imply any special 
 difference in their chemical composition. These physical differences depend upon the 
 conditions under which solidification was effected, whether gradual or rapid. In the 
 former case the molten mass would develop erystals, in the latter it would remain 
 amorphous; it would, in fact, result in a more or less perfect glass. In these natural 
 glasses it is, however, common to find crystallites and crystals, the former usually 
 developed very completely, the latter less perfectly formed asa rule, since they generally 
 present rounded boundaries, or their angles, if any exist, also appear rounded.” 
 
 From Rutley’s remarks, as above quoted, and from the fact that the whole 
 subject of the classification of rocks is so beset with pitfalls, it appeared safer to 
 provisionally place the Mackay quartz-trachytes under the rhyolite group.* Subse- 
 quently they may be re-ciassed, when the rock collections are more representative. 
 I have no wish to evade the eclassificatory difficulty, but after quoting Professor Hutton’s 
 remarks on the difficulty of classifying rocks, I shall leave the reader to judge of the 
 wisdom of waiting for further developments. He says + :—‘ The confusion, indeed, has 
 become so great that some petrologists discard names as much as possible, and in their 
 place give a list of the minerals composing the rock. This plan has the merit of not 
 adding to our confusion, but it will not help us out of it. And when we read of 
 ‘ plagioclase-augite-olivine-mica rock,’ or of ‘felspar-pyroxene-magnetite-garnet rock,’ 
 our patience is well-nigh exhausted. 
 
 “‘ Natural.science progresses by the comparison of objects, and when objects are 
 numerous they must be named, if for no other purpose, still for indexing; so that an 
 observer may readily find descriptions of similar objects for comparison, and ascertain 
 what others have said about an object similar to the one he may be studying. As books 
 get more and more numerous a uniform nomenclature becomes of more and more 
 importance from the single point of view of indexing, and until some uniformity in 
 rock nomenclature has been attained we cannot expect any very great advance in 
 petrology.” 
 
 The rhyolites are poorly represented in this Collection, but are generally typical. 
 Particular attention is drawn to the Nell Isle sample, No. 108, which is so beautifully 
 characteristic that the artist has drawn it in three different lights. For those readers 
 to whom the subject is new they afford excellent illustrations of fluxion-structure and 
 rock-texture. 
 
 The Mackay sample, No. 58, shown on Plate No. 62, fig. 2, is also a good type of 
 the group. 
 
 The Mackay quartz-trachites are fairly interesting, but as type rocks they are 
 not above the average. What makes them of special interest is that they illustrate 
 Departmental work, having been prepared in London by a professional, and are about 
 as thin as rock-sections can possibly be, which is the desideratum in petrography. 
 
 The Cloncurry obsidian ealls for special notice, owing to its anisotropic pro- 
 perties. It faintly polarizes between crossed nicols, and it is remarkable that the 
 section is free from microlites, crystal growths, and gas-pores. Zirkel says such vol- 
 canic glasses are extremely rare. Finally, the single example of tachylyte merits a 
 
 
 
 
 
 * Mr, Maitland informs me that the Mackay trachites exhibit, in the field, almost all degrees of 
 texture, from coarse trachites at one end of the series to nearly trachite glass at the other. 
 
 + ‘The Eruptive Rocks of New Zealand.” A Paper read before the Royal Society of New South 
 Wales, 7th August, 1889, and published in their journal, vol. xxiii., p, 102. 
 
733 
 
 passing notice. Had circumstances been more kindly, the yellow glass would have 
 teemed with crystals and crystallites. After reading Professor Judd’s last Paper on 
 “The Rejuvenescence of Crystals,” one cannot help musing on the barrenness of a 
 Soil so capable of sustaining crystal life. 
 
 BASALTS. 
 
 But little description is necessary of this group of rocks, for the name is cld and 
 the rocks are familiar under that name to most. There are three varieties of basalts: 
 basalts proper, anamesites, and dolerites ; names denoting difference of structure or 
 texture rather than mineralogical variation. 
 
 I. Basalt proper is compact, amorphous, often semi-vitreous, breaking with a 
 perfectly conchoidal fracture. 
 
 II. Anamesite (from avé-yecos, intermediate) is uniformly crystalline, but close- 
 grained, the crystals being very small. 
 
 IIT. Dolerite is coarsely crystalline, the word signifying: deceitful, a name 
 suggested by the difficulty of distinguishing it from certain Plutonic rocks. 
 
 Zirkel classifies the basalts mineralogically into— 
 
 1. Felspar-basalts. 
 
 2. Nepheline-basalts. 
 
 3. Leucite-basalts. 
 
 Mohl divides the members of the basalt group into— 
 
 1. Magma-basalts, with a colourless or brown-glass matrix. 
 
 2. Plagioclase-basalts, containing notably plagioclase and occasionally nephelene 
 in addition to the essential augite, magnetite, &e. Leucite seldom. 
 
 3. Nepheline-basalts, containing notably nepheline, and sometimes leucite, in 
 addition to augite, magnetite, &c, Plagioclase rare or absent. 
 
 4. Leucite-basalts. 
 
 5. Hauyne and nosean-basalts. 
 
 6. Mica-basalts. 
 
 Rutley says :— 
 
 “In microscopic sections of basalts which have undergone partial decomposition, 
 the olivine and augite crystals are often merely represented by pseudomorphs of green 
 matter, which is serpentine or some other hydrous silicate. The augite in basalts is 
 generally rich in glass enclosures. Steam pores and fluid lacune are also of common 
 occurrence in them. The olivine sometimes appears in tolerably well-defined crystals ; 
 but it is more usually in roundish grains, or in granular aggregates. The latter are 
 sometimes of considerable size, and occasionally show, in external configuration, that 
 they are large, rudely-developed crystals. The plagioclase basalts are of more frequent 
 occurrence than any of the other rocks belonging to the basalt group.’’* 
 
 The most interesting of the basalts, described in the foregoing pages, is the 
 leucite-basalt from the Normanby Reefs of the Cooktown District. This is the first 
 oceurrence of leucite noted in Queensland. The Mineral Census of Australasia t 
 (including only the Colonies of New South Wales, South Australia, Queensland, and 
 New Zealand) records only three places where it has been recognised. They are— 
 
 1. Leucite-basalt, Castle Point, New Zealand. 
 
 2. Byrock, County Cowper, N.S.W. (T. W. E. David and W. Anderson.) 
 
 3. El Capitan, County Cambelego, N.S.W., in a basaltic lava sheet. 
 
 
 
 
 
 * F, Rutley. The Study of Rocks, page 254. 
 + Report of Committee, No. 7; Mineral Census of Australasia, Proc. Austr, Assoc, Adv. Sci., IL., 
 
 1890, pp. 213-273, 
 
734 
 
 In connection with the subject of leucite rocks, Zirkel says :— 
 
 “More than twenty years ago, Alexander von Humboldt published his 
 conclusion that leucite was a mineral only found in Europe; and it is rather curious 
 that this casual remark has not been disproved until very recently. This mineral, up 
 to the year 1868, was only known as a constituent of several lavas of Italy, of the 
 Laacher See, and of the Kaiserstuhl, in Baden. Since that year, it has been 
 discovered to be a microscopical ingredient of many basalts of Saxony, Bohemia, the 
 Thiiringer Wald, and the Rhén Mountains, occurring in unexpected frequency. But 
 all these localities were European; so the remark still held good; and the other 
 extra-European basic rocks, examined in large quantity, were never found to contain 
 leucite. 
 
 “In 1874, Vogelsang discovered an Asiatic leucite. It occurred in a basaltic 
 rock from the Gunung Bantal Soesoem, upon the small island of Bawean, north of 
 Java. . 
 “ And now the microscopical study of the rocks of the Fortieth Parallel estab- 
 lishes the existence in America of the most classicl eucite rocks. Moreover, these 
 rocks are richer in the mineral than any occurrence in the Old World, besides which 
 their general composition is very peculiar. Leucite was always considered, as is well 
 known, one of the most perfect members of the regular system, until, in 1872, G. vom 
 Rath stated that it belonged to the tetragonal or quadratic system, the apparent 
 icositetrahedron being a combination of (P,P,). The colourless crystals, which 
 geverally show in the section a more or less regular or rounded octagon, have the 
 peculiarity of containing a great quantity of strange little crystals and grains grouped 
 into a small central heap or (which is more often the case) concentric zones, of which 
 the sections are also octagonal or roundish. These corpuscula, which are supposed to be 
 intruded into the leucite, are, instead, situated on the surface of the leucite forms or 
 globular figures.”’* 
 
 Teall states that leucite has not yet been found in Britain.t 
 
 The “ Mitre Rock” sample from New Guinea is to be noted on account of the 
 abnormally large size of the augites, many sections of which happen to be cut parallel 
 to the plane of symmetry (OLO) or ©P». The other Queensland basalts of this 
 collection call for no special remark, although some, like the Herberton basalts, are 
 highly typical rocks. But the three samples from New South Wales (two from 
 Bathurst, and the other from Mount Sassafrass) are, par excellence, the basalts of the 
 whole collection. Some of Zirkel’s excellent drawings in “ Microscopical Petrography,” 
 quoted above, might almost be used to illustrate their textures. 
 
 The dolerites of the Sellheim River are so rich in apatite that one cannot fail to 
 be struck with the sections, with their brilliant little water-clear hexagons appearing as 
 black as ink, of course between crossed nicols. 
 
 Lastly, the Mount Kinchant (Mackay) sample is of interest, as it is pretty fresh, 
 and its felspars very much banded and pellucid. 
 
 DIORITES AND PORPHYRITES. 
 
 Diorite proper is a crystalline-granular mixture of plagioclase felspars and 
 horneblende, while porphyrite is characterised by a granular base of plagioclase felspars, 
 and either hornblende or augite, in which base are developed larger crystals of the same 
 minerals, There is, therefore, a mineralogical connection between the two groups, 
 though structurally they are different. Professor Hutton uses the word “ porphyritic’’ for 
 
 
 
 
 
 * “* Microscopical Petrography,” p. 259. 
 t+ “British Petrography,” Note on Fig. 2, Plate xli. 
 
735 
 
 describing a rock texture. Lyell uses the word in describing that granite in which large 
 crystals of felspar, usually orthoclase, are sometimes scattered through an ordinary 
 base of granite. 
 
 I have measured crystals in the porphyritic grarite of Dartmoor two inches in 
 length, and Lyell mentions crystals measuring three inches in length in the porphyri'ie 
 granite of the Land’s End.* 
 
 The rocks are so variously named by different writers that it is not easy to be 
 precise in definition. For instance, Judd, after examining some of my sections, states in 
 a letter to me that ‘the rocks named ‘Queensland granite’+ belong to the class of 
 quartz-diorites (tonalites) which appear to be very abundant in Queensland. They were 
 recognised as such by the late Mr. R. Daintree.” 
 
 The diorites are very poorly represented in the Collection. They call for no 
 summarising. 
 
 In the rocks grouped under the head of porphyrites it is otherwise. The 
 Croydon series is of interest, as are also the two, Nos. 79 and 80, from the Great 
 Northern Tin Mine, Herberton. The sections from this porphyrite dyke show how 
 much more the quartzes have suffered from erosion at the 3800-feet level than is the 
 case with the samples from the surface. No. 82, from the Peak, New South Wales, is 
 remarkable for the size of the felspars. The artist had to draw this really striking 
 section on a very much larger surface in order to illustrate the two sets of felspar twins 
 (Vide Plate 60). 
 
 I should have liked to have learned something from the Gympie “ greenstone” 
 sections; but neither Mr. Rands nor myself came to any definite conclusions. In Mr. 
 Jack’s ‘* Mineral Wealth of Queensland,” published in 1888, he says :—‘‘ The greenstone 
 of Gympie has long formed a subject of controversy . . . . evenin microscopic 
 sections, these rocks are much altered and ‘ masked’ by viridite.” 
 
 INDEX TO PLATES. 
 
 Plate 60.—Intrusive Dyke-stone from the Peak, New South Wales. OC. S. Wilkinson’s 
 Collection. With polarizer only, magnified 50 diameters. 
 
 Plate 61, Fig. 1.—Rhyolite.—Nell Island, New Guinea Sir W. Macgregor’s Collection. With 
 polarizer only, magnified 42 diameters. 
 
 a Fig. 2.— hs Nell Island, New Guinea. Sir W. Macgregor’s Collection. With 
 parallel nicols, magnified 42 diameters. 
 
 Plate 62, Fig. 1.— i Nell Island, New Guinea. Sir W. Macgregor’s Collection. With 
 crossed nicols, magnified 42 diameters. 
 
 As Fig. 2.— + Hamilton, Mackay, Queensland. A. G. Maitland’s Collection. 
 With crossed nicols, magnified 27°5 diameters, showing fluxion- 
 structure. 
 
 Plate 63, Fig. 1.—Tachylite—Queensland. .R L. Jack’s Collection. With polarizer only, 
 
 magnified 27°5 diameters. 
 
 Fig. 2.—Quartz, with tourmaline crystals —With polarizer only, magnified 42 
 
 diameters. Cooktown. A.J. Madden, Esq., collector. 
 
 Plate 64, Fig. 1.—An interesting unnamed rock, from Cape Upstart, collected by R. L. Jack, 
 partially prepared by him and finished by the Author. Mr. Jack 
 has no more of the rock left, the whole chip having been ground 
 away. Between crossed nicols, magnified 27°5 diameters. 
 
 3” 
 
 
 
 
 
 
 
 * Sir Charles Lyell. Elements of Geology, 2nd Edition, p, 556. 
 + The granites referred to are from Cooktown, John Bull, Ravenswood, and at about 700 feet down 
 the Queen Block Extended shaft, Charters Towers. 
 
736 
 
 Plate 64, Fig. 2.—Pitehstone Sheffield, Tasmania. R.L. Jack’s Collection. With polarizer 
 only, magnified 42 diameters. 
 
 Plate 65, Fig. 1.—Basalt.—Russell River, Queensland. R. L. Jack’s Collection. With 
 crossed nicols, magnified 50 diameters. 
 
 % Fig. 2.—Augite crystal showing twinning. Gympie, Queensland. W. H Rands’ 
 Collection. With crossed nicols, magnified 50 diameters.* 
 
 Plate 66, Fig. 1.—Obsidian.—New Guinea. Sir W. Macgregor’s Collection. With crossed 
 nicols, magnified 50 diameters, showing fluxion-structure and 
 quartz crystals full of gas pores. 
 
 3 Fig. 2.—Basalt, Burdekin, Queensland. A. W. Clarke’s Collection. With crossed 
 nicols, magnified 27°5 diameters. 
 
 Plate 67, Fig. 1—Hornblendic dyke running through the Durham Mine, Etheridge, Queens- 
 land. R.L. Jack’s Collection. With polarizer only, magnified 
 27°5 diameters. 
 
 5 Fig. 2.—Zeolitic mineral vein running rudely parallel to a calespar vein in a red 
 granite. Rainbow Claim, Charters Towers, Queensland. 
 Natural size, drawn from a polished face. 
 
 Plate 68.—Daunton’s Hill, Upper Cape River, Queensland. W. H. Rands’ Collection. 
 Between crossed nicols, magnified 42 diameters. Mr. Rands 
 states that quartz leaders running through this rock cease to 
 earry payable gold. (No. 34 in Appendix.) 
 
 Notes to Prats 67, Fig. 2 
 The Analysis of the red zeolite shown in this Plate is as follows :— 
 $i0, oe es Rt ine bis Se ae ane 47°0 
 Hie 0 ee sale Fc $0 13°7 
 This hyde silicate is common on is Chanter. Towers Gold Field, occuring in the 
 joints of the granite. Various samples have been analysed. The following are selected from 
 many others :— 
 
 1. From the Queen Block Extended, 700 feet vertical i 
 
 
 
 
 
 Silica ... ; one RIC ae ‘ee A io 46°25 
 Alumina be sj ™e ie ie ds aa 27°35 
 Ove Se ose age er, act oes sa races 
 Lime ... ch nn He a aa 13:95 
 Water (by ry ey rs or rae ee 13°47 
 
 101°02 
 
 2. From the Mary aren occurring at a map e of 300 feet. 
 
 NiO. : Bee Bee 49°04: 
 Ab, 0; aah tae 436 oe wea Be We 26°64: 
 Caio é me et ne See Ng Pa 
 H,O (by ignition £3, bas ne er ‘is ie 13°30 
 On as ; tee re a as we 554 Traces 
 
 101°22 
 
 3. From the Mexican Claim, at a low fa 
 
 SiOZames ae x00 ani ac are se 47°24 
 Al OR ns an sik mf ods Nea wae er, 26°64 
 CaO ce “0 ae ee nies ate se na 12°95 
 HOw: ns a ee we rey yf vet 1420 
 Fe, Q,..; A se Ae aes Sen i's .. Traces 
 
 101°03 
 
 
 
 * Mr. Rands has favoured me with the following description of this rock, which he names Diabase- 
 porphyrite :— 
 
 “A dark-green, interbedded, amygdaloidal rock. Amorphous ground-mass, with porphyritic crystals 
 sharply defined, and for the most part showing twinning. Magnetite in small grains, and calcite. Amygdules 
 filled with carbonate of lime.” 
 
 + Vide Proc. R. Soc. Queensland, 1887. 
 
737 
 APPENDIX. 
 
 A Suorr Descriprion or Some or THE CapPE River Rocks ExaMIneD 1N Tuin SEcTIONS 
 UNDER THE Microscorr. By Wixi1am H. Ranps. 
 
 1. A dark-coloured, fine-grained hornblende schist, from Union Reef, near Mount 
 Davenport. The slide consists almost entirely of green hornblende and quartz. The quertz 
 contains enclosures of apatite and other minute enclosures. In a section cut transversely to 
 the cleavage the longer axes of the hornblende have a inear arrangement. 
 
 2. A white mca schist, from Mount Davenport. The slide consists chiefly of quartz in 
 small grains, with mica. In a section cut transversely to the cleavage of the rock the mica is 
 arranged in layers. 
 
 3. A hornblende schist, from the southern slope of Mount Davenport. Green hornblende, 
 beautifully cleaved, with bands consisting of grains of quartz. There is more hornblende 
 than quartz in the section. Magnetite occurs in grains. 
 
 4. A red fine-grained granite, from Mount Frank. Quartz occupies the larger portion 
 of the slide; itis full of minute enclosures. Plagioclase felspar, which is much kaolinized. 
 White and black mica. - The slide contains numerous large specks of magnetite. 
 
 7. Felsite, from dyke in schists, Pentland Reefs. The rock consists of a fine decom- 
 posed felspathic ground-mass, with ferrite throughout it. 
 
 8. A red, medium-grained granite, from Homestead Range. The section is rather thick 
 and indistinct. The slide contains crystals of plagioclase felspar, and also beautiful star-shape 
 spherolites of plagioclase felspar; gwartz, with enclosures of magnetite; mica; and specks of 
 magnetite throughout the slide. 
 
 12. Dolerite, from dyke near Specimen Creek, Mount Remarkable. This slide is very 
 thick, and the only minerals that can be determined are decomposed felspar and small specks 
 of augite in a semi-crystalline ground-mass. 
 
 15. Graphic granite, from dyke near Specimen Creek, Mount Remarkable. The slide 
 consists of elongated plates of quartz in felspar. All the quartz extinguishes simultaneously ; 
 and the same is the case with the felspar. 
 
 16. Quartzite, from Golden Hill, near Mount Remarkable. This rock consists almost 
 entirely of semi-rounded and irregular-shaped granules of quartz, containing numerous 
 enclosures, among which are small acicular crystals, probable apatite. There are crystals of 
 magnetite in the slide, and some ferrite. 
 
 17. Quartz felsite, from a dyke on the ridge north of Mount Remarkable. The slide 
 consists of an amorphous ground-mass, with blebs of quartz throughout it. It contains a little 
 ferrite. ; 
 
 22. Gabbro,a dark crystalline rock from a dyke near Specimen Creek. This slide is 
 made up of diallage, which is very feebly dichroic, a plagioclase felspar, and mica. Small 
 grains of magnetite occur throughout it. 
 
 24. A white kaolinized felsite, from Running Creek, Norwood. It consists of an 
 amorphous ground-mass, with minute grains of quartz throughout it, which have a banded 
 structure. ‘There are also small grains of magnetite, and a few porphyritie crystals of felspar. 
 
 25. A reddish-brown fe/site, from Running Creek, Norwood. The slide shows a fine 
 felspathic ground-mass, with minute lath-shaped crystals of felspar throughout it. Porphyritic 
 erystals of plagioclase felspar, with enclosures of apatite and magnetite; a few porphyritic 
 erystals of orthoclase felspar. Crystals of magnetite occur in the ground-mass. Ferrite occurs 
 in considerable quantity, giving the red colour to the rock. The rock shows a beautiful perlitic 
 structure. 
 
 26. A purplish Jelsite or porphyry, from Running Creek, Norwood. The rock consists 
 of a dark-coloured amorphous ground-mass, containing a large amount of ferrite, and showing 
 in parts a well-marked fluxion-structure. There are numerous porphyritic crystals of 
 decomposed fée/spar, most of which were rubbed away in the preparation of the slide. Large 
 crystals of magnetite occur. 
 
 27. Dolerite, from a dyke in Chinaman’s Gully, Sandy Creek. A dark, fine-grained 
 rock with a spherulitic structure on weathering. A felspathic ground-mass full of small 
 
 2X 
 
738 
 
 lath-shaped crystals of felspar, and also magnetite in both large and small grains. The 
 pyroxene element has been changed into viridite. There are a few larger crystals of both 
 orthoclase and plagioclase felspar. a 
 
 30. Hornblende schist, from Sandy Creek. A very beautiful slide containing green 
 hornblente, having a linear arrangement, and showing very perfect cleavage parallel to the 
 plane of symmetry and faces of the prism. These crystals contain enclosures of apatite and 
 epidote. Beautifully twinned crystals of plagioclase felspar, some of which appear to have had 
 a secondary growth; they contain enclosures of apatite. A few solitary crystals of orthoclase 
 JSelspar. There are a few specks of quartz ; magnetite is very rare. 
 
 31. Garnetiferous granite, from the Pentland Range, at the head of Sandy Creek. The 
 slide is much broken. The minerals that can be distinguished are—Quwartz, containing 
 prismatic enclosures of apatite ; plagioclase felspar ; mica, and garnets. 
 
 33. Hypersthene rock. A dark-coloured, highly crystallised rock, from a dyke on 
 Daunton’s Hill, Upper Cape. Hypersthene is the principal mineral. It is a green mineral, 
 possessing strong pleochroism; the cleavage is prismatic. The mineral extinguishes parallel 
 to the planes of cleavage. It contains several hexagonal enclosures of apatite, and also of 
 quartz; streaks of quartz follow the cleavage planes. It also contains enclosures of magnetite. 
 Quartz in large plates is the next mineral in importance; it is full of very minute enclosures. 
 Brown mica oceurs in the hypersthene, and also in a semi-transparent iron compound— 
 leucoxene, of which mineral there is a large amount in the slice. 
 
 34. Hornblende schist, from Daunton’s Hill, Upper Cape. A crystalline rock resembling 
 a coarse diorite, except that the hornblende occurs more or less in layers. This is the rock in 
 contact with which the leaders on Daunton’s Hill ceased to carry gold. The rock is made up 
 to a large extent of very beautifully twinned crystals of oligoclase felspar, full of small 
 hexagonal enclosures of apatite, and also enclosures of leucowene. Hornblende, well-cleaved, 
 and containing also enclosures of apatite. Quartz in small blebs. Magnetite changing around 
 its edges into lewcoxene. : 
 
 35. A highly erystalline schist, from Mount Elvan, Upper Cape. Quartz is the principal 
 mineral ; it contains enclosures of small garnets. Entwined around the quartz is green 
 hornblende. Plagioclase felspar. Very small garnets occur throughout the rock. 
 
 36. A fine-grained, grey micaceous granite, from Mount Elvan, Upper Cape. The 
 minerals in the slide are—Plogioclase felspar, some of which is much decomposed. Well- 
 cleaved white mica ; and quartz with acicular crystals of apatite, and other minute enclosures. 
 
 38. A purplish porphyry, from the Cape River, near the Pot-hole Lead, Upper Cape. 
 It consists of an amorphous ground-mass, showing fluxion-structure, and full of ferrite and 
 magnetite. It contains porphyritic crystals of plagioclase felspar. 
 
 40. Olivine basalt, from Mount Black. A compact black rock, possessing polarity. ‘he 
 slide shows a microcrystalline ground-mass, containing numerous specks of magnetite, with 
 crystals of olivine, a few crystals of felspar, and specks of augite. 
 
 42, Olivine basalt, from the Tableland, Oxley Creek, a somewhat scoriaceous basalt 
 containing zeolites. The rock consists of an interlaced mass of acicular crystals of felspar, 
 with crystals of olivine throughout it. Some of the olivine crystals are much decomposed 
 around their margins, and along cracks in the crystals. Magnetite is comparatively rare. 
 
 43. Basalt, from the Basaltic Wall, Lolworth. A highly scoriaceous basalt. The rock 
 was a difficult one to cut, and the slice is very small. It shows an interlaced mass of crystals 
 of plagioclase felspar, with small specks of olivine. 
 
 Norr.—The microscopial slides described above were prepared for me by Mr. A. W. 
 Clarke. 
 
APPENDICES. 
 —_—~<}—--- 
 
 APPENDIX I. 
 
 AGE OF THE MOUNT ALBION AND CHILLAGOE BEDS. 
 
 My Colleague leans to the opinion (See pp. 118-120) that these beds are equivalent to 
 those of the Palmer and Hodgkinson, whick he provisionally refers to the Gympie Series, but 
 remarks on the paucity of organic remains. Mr. William Thompson, Government Mineral- 
 ogical Lecturer, appears to have been more fortunate in the discovery of fossils, and says*:— 
 
 “Owing to the alteration the limestone has undergone the fossil remains are generally 
 so crystalline that beyond the outline nothing indicative of the original organic structure 
 remains. Corals and encrinite stems are everywhere common, though, as a rule, very 
 imperfect; in places, however, bands of rock exist containing remains more or less distinct, 
 and from these several fossils have been derived. Amongst them are examples of Aviculo- 
 pecten and Huomphalus, Cyathocrinus, Lithostrotion basaltiforme, Zaphrentis, Cyathophyllum, 
 and numerous cther corals. Two or three poor specimens of what appear to be small Trilobites 
 and a fine example of an Annelid were also found. I would remark that these are named 
 with reserve; as I have no means of comparing them either with recognised specimens or 
 diagrams.” 
 
 The assemblage of fossils named by Mr. Thompson might be present in a Carboniferous 
 deposit, but I have never seen Lithostrotion basaltiforme in Australia, nor have I seen 
 Cyathophyllum in the Queensland Permo-Carboniferous. Zaphrentis, however, does occur in 
 the latter, as well as close allies of Cyathocrinus. Allowing for Mr. Thompson’s “reserve” in 
 naming the fossils as he had done—a reserve which would be justifiable on the part of any 
 Paleontologist without “means of comparing them either with recognised specimens or 
 diagrams ”"—the supposition of the Permo-Carboniferous age of the beds in question appears 
 still to be the most probable. 
 
 ° E. 
 APPENDIX II. 
 THE GLASSHOUSE MOUNTAINS. 
 
 The difficulty of determining the nature of the rock composing these mountains is con- 
 siderably increased by the conflicting testimony of various writers on the subject. Mr. Stutch- 
 bury, in 1854, regarded the rock as a “ metamorphic sandstone ” (See page 73). The Honourable 
 A.C. Gregory (See page 5) referred to it, in 1879, as an “ outburst of porphyry.” JT inally, 
 the Rey. J. EK. Tenison Woods, in 1888, in his Paper on the Desert Sandstone,} published 
 a view of “ Prismatic Basalt, Glasshouse Mountains,” but without any reference in the text. 
 
 Recently Mr. Henry G. Stokes has. presented to the Geological Survey a series of 
 specimens collected in the Mountains themselves, from which it appears that the staple rock is 
 trachite, although it is possible that basalt or porphyries may be present as intrusive masses. 
 The mountains are accordingly marked in the Geological Map as trachite. J 
 
 APPENDIX III. 
 ARTESIAN WELLS. , 
 
 Referring to the remarks on page 418, regarding the possible diminution of the supply 
 from Artesian Wells, the Charleville Well furnishes some suggestive facts. 
 
 In 1890 the pressure per square inch had increased from 95 lb. to 100 lb., and the 
 temperature was 106° Fahr.f On 10th July, 1892, the pressure had decreased to 87 lb., and 
 the temperature to 101°. The last-mentioned measurements were made by Mr. J. B. Henderson, 
 Hydraulic Engineer, in my presence. 
 
 J. 
 * In Annual Report of the Department of Mines for 1891, p. 185. Brisbane: by Authority : 1892, 
 
 + Proc. Roy. Soc. N. 8. Wales, 
 t See page 427, 
 
 
 
740 
 
 APPENDIX IV. 
 
 ORGANIC REMAINS, EIGHT-MILE PLAINS, NEAR BRISBANE. 
 
 In stating (p. 608) that remains of the Extinct Mammalia had been discovered in this 
 locality, I was under the impression that Mr. C. W. De Vis had obtained, among others, 
 remains of an extinct Species of Wombat, but Mr. De Vis informs me that I was mistaken. 
 The only organic remains from the Hight-Mile Plains yet identified are those of Ceratodus 
 Fosteri and Pallimnarchus pollens—a fish and a reptile, both of living species. The case, then, 
 still stands thus, that the known remains of extinct mammalia have all been derived from 
 comparatively high levels, whatever significance the fact may have. y 
 
 APPENDIX V. 
 EOCENE BEDS IN VICTORIA. 
 The following should have been added as a footnote after the word “ Miocene,” p. 575, 
 line 29 :— 
 “ Professor R. Tate, on ihe other hand, regards the fossils from the Schnapper Point 
 clays, Port Phillip, as of Eoceneage. Journ. R. Soc. N.S. Wales for 1888 [1889], xvii., p. 242.” 
 
 J. 
 APPENDIX VI. 
 
 DARR RIVER DOWNS BORE No. 3. 
 
 In a paragraph on p. 424, the depth of this bore is given as 2,700 feet, and the daily 
 overflow as 50,000 gallons. The bore has since been continued to 3,530 feet, and is therefore 
 the deepest in the Australian Colonies. (See “ Muckadilla Bore,” p. 428.) Mr. Fiskin, one of 
 the owners of the Station, states that the “bottom” is sandstone, that the daily overflow is 
 500,000 gallons, and that the temperature of the water is 172° Fahr. J 
 
 APPENDIX VII. 
 LACERTILIAN REMAINS ON SUTTOR RIVER. 
 An additional locality for remains of the extinct Lacertilia has been furnished by Mr. 
 De Vis, who informs me that a Vertebra of Megalania, from black soil on the bank of a lagoon 
 
 at Mount Lookout, near the head of the Suttor River, was sent to him by Mr, Peter Murray 
 about twelve years ago, and is now in the Queensland Museum. 
 J. 
 
 APPENDIX VIII. 
 LIST OF FOSSILS OF THE BURRUM BEDS, WITH THEIR SYSTEMATIC POSITIONS. 
 In consequence of the introduction of Phyllopteris Feistmanteli into my Colleague’s List 
 
 after Chapter X XIII. was in type, the following corrections are necessary :— 
 Page 311. After the paragraph on Teniopteris (Angiopteridium) Daintreet, insert :-— 
 
 “ Genus—PHYLLOTHECA, Saporta. 
 
 “ PHYLLoPTERIS FristMantsE.i, Lth. fil. 
 * Zoc. Styx Coal Field (Burrum Beds). Occurs also at Stewart’s Creek, Rockhampton 
 —(Ipswich Beds).” 
 Page 312. In the Synopsis, after Alethopteris australis, Morr., insert :— 
 “* Phyllopteris Feistmanteli, Eth. fil.” 
 And the last two lines should read :— 
 “ Of the thirteen species above named, five are common to the Ipswich Formation, and 
 the remaining eight are peculiar to the Burrum Formation.” J 
 
741 
 
 APPENDIX IX. 
 DESCRIPTIONS OF THE SPECIES OCCURRING IN THE BURRUM FORMATION. 
 
 In consequence of the introduction of the new species Phyllopteris Feistmanteli after 
 Chapter XXIV. was in type, the following addition becomes necessary :— 
 Page 315. After the paragraph on the Genus Trichomanites, insert :— 
 
 * Genus—PHYLLOPTERIS, Saporta, 18—. 
 
 “ PHYLLOPTERIS FrtstManTELI, th. fil. 
 
 “Obs. For description of the species, see ‘ Ipswich Beds’ (p. 375). 
 “Loc. Styx Coal Field (Burrum Beds). Occurs also at Stewart’s Creek, Rockhampton 
 —(Ipswich Beds).” 
 E. 
 
 APPENDIX xX. 
 GEM-BEARING DRIFT AT WITHERSFIELD. 
 
 For an account of a Drift, probably of Tertiary age, containing Sapphires, Oriental 
 Emeralds, Zircons, &c., see Report by the Writer ‘On Sapphire Deposits and Gold and Silver 
 Mines near Withersfield.”” Brisbane: by Authority: 1892. 
 
 J. 
 

 
 7 
 = 
 
INDEX TO PERSONS QUOTED OR REFERRED TO. 
 
 SS SSS 
 
 Page. Page. 
 
 ABICH, — ... 244, 461 Bronn, H. G. ; fe . 278, 448, 452 
 Adams, A. veo. G9 Brot, A. d eA ... 606, 632, 642, 693 
 Adams, H. . . 606, 632, 644 Brow ra aE vl ; 376, 408, 433, 450, 451, 
 Adams, H. and A. . a 000 454, 456, 457, 467, 473, 
 Adams and Angas... 600, 632, 642, 644 A79, 493, 549, 552, 632 
 Adanson, M. . 485, 573, 643 Brown, R. ... A A i oe 371 
 Agassiz, A. ... 692, 697 Brown, W. H. a un oe en, SVE, 
 Agassiz, L. .... 84, "287, 296, 397, 413, 446, "480, Bruck, Ludwig ; 428, 630 
 481, 503, 504, 559, 567, 571, 646 Bruguiere, J.G. ... ; 264, 444, 
 
 Allport, J. E. ote .. 668 447, 462, Ae 562, 
 Allport, Samuel... aes ; 79, 145 567, 635, 642, 696 
 Anderson, William 542, 598, 601, 735 Buch, Leopold von we 44, 67, 03, 242 
 Aplin, C. D’Oyley H. See Cals; 20, 34, 72, 73, Buchanan, W. ee =a : OS 
 74, is 2, 323, 324, 595 Buckland, T. fan ee xa ees! 
 
 Ayrchiac, E. J. A. a’ ; 289 Burkitt, J. ... ae aft . 407, 503, 506 
 Archibald, R. ay tee ae soa AB, Burrows, N. H. ... a Be me hs: 
 Astier, J. E. ay Be Say rie OL, Bus, B. du ... ies <n ee Ve OOS 
 Austin, T. and T. ... are ae sho AO Busk, G. 221, 441 
 Battery, F. M. aa nae oe sag OS! CAMPBELL, H. “ae a ne pe 00S 
 Baily, W. H. sv ae seks tae 405 Canefri, T. ... Se 693, 694 
 Barker, R. T. 43 is Sine Sa a! Canham, J.. 456, 491 
 Barrande, Joachim ae hs soo SY Carpenter, P. H.. ... “6 ., 209-218, 440 
 Barrow, G. H. ber see ie me Bae Carron, Wm. an ee ’ eee eb Al 
 Bate, C. Ste ee ose i .. 298 Carruthers, W. ~ 196, 198, 313, 
 Bauer, Hare nbc Ges aa Me tOS 315, 351; 352, 353, 354, 
 Bayle, EH. ... ave ne A 288 356, 362, 368, 367, 368, 
 Bean, W. ... vee a : 317, 360 374, 378, 384, 386, 392 
 Beek, 1. O.--.. ar a me . = 646 Carson and Sutherland .. 468, 464, 491, 
 eget Rae! OA ce a eis RS SIS * 495, 496, 498, 
 Bell, T. sae S00 ee oH 635, 639 506, 508, 509 
 Bennett, G. 505, 642, 648 65z, Carter, H. J. 437, 438, 439, 505, 507 
 667, 668, 673, 676, 677 Chandler, J. 8. : 456, 486, 491 
 
 604, 647, 648, 649, 667, 
 668, 673, 674, 677, 680, 681 
 
 Bennett, George F. 
 
 Bennett, Israel Bae 17, 18 
 Berger, Julius von... 401, 402, 403, 407, 468 
 Berjeau, Charles... Fe KVL: 
 
 690, 693, 694, 695, 697 
 . 295, 449, 453 
 
 Beyan, Theodore 
 Beyrich, E... 
 
 Billings, HE. ... 58 58 
 Blainville,H. D. de... 52, 245, 312, 319, 488, 492 
 Blake, J. F. Sac 69 
 Blumenbach, J. F.... oT Hef son ake! 
 Bonaparte, C. L. ... Bb she ..» 658 
 Bonwick, James... Ro ave so OY 
 Boulenger, G. A. ... sls ue .. . 648 
 Bowerbank, J. S&S. ... out 50 436, 438 
 Boyd,— ... Shp 5 505 sae 668 
 
 Brand, A. ... ha ae , ae R406 
 Braun, F. Ad: 311, 312, 317, 318, 
 
 352, 353, 380, 381 
 
 Brazier, John oon See eee 473, 477, 483, 
 578, 698, 695, 698 
 
 Breynius, J.P... _ 292, 293, 502 
 Brisson, J. ... “se a as a kai 
 Brongniart, A. 159, 175, 178, 179, 189, 
 190, 193, 194, 197, 311, 314, 
 
 317, 351, 352, 353, 356, 365, 
 
 366, 371, 376, 378, 379, 380, 
 
 381, 384 385, 386, 558, 642 
 
 
 
 
 
 Clarke, A. W. alae tS, 11, 14, 27, 
 128, 594, 599, 699 
 Clarke, W. B. a Eis ee Tel Oar 
 35, 59, 72, 92, 195, 390, 391, 
 392, 394, 396, 435, 436, 439, 
 440, 442, 444, 445, 446, 44:7, 
 448, 449, 451, 456, 457, 458, 
 459, 460, 462, 466, 467, 468, 
 469, 470, 471, 475, 476, 477, 
 479, 480, 481, 483, 484, 485, 
 486, 487, 488, 489, 501, 511, 
 512, 520, 553, 606, 658, 661 
 Clifford, J. D. nae ; eo 200 
 Coane and Clarke .., ae 10, 584 
 Conrad, T. A. 269, 276, 460, 482, 486, 
 562, 606, 632, 633, 642 
 
 Conybeare, W. D. .. 2 508, 510 
 Cooper, D. ... a 664, eee 677, 678 
 Coquand, H. ts Gc ww 445 
 Cotter, A. S. - 608, 659, 661 
 Cox, J. C.*., 491, 636, 640, 643, 645 
 Cramieri, G. fe oe 407 
 Crépin, Be Bc oe Bae seg Ghats) 
 Crummer, H. J.W. an a ae DOO 
 Cullen, Charles... fas eg were (oS 
 Curran, J. Milne Ho 468 367, 368 
 Cuvier, F<. “ “ a OOO) 
 Cuyier, G. ... - Pap 503, 663 
 
744 
 
 DAINTREE, Richard iii., vi., viii., xiv., 
 
 INDEX TO PERSONS. 
 
 Page. 
 XVii., 
 15, 20; 22, 23, 28, 31, 32, 35, 
 36, 50, 51, 58, 61, 62, 72, 79, 
 95, 128, 129, 137, 1438, 158, 
 169, 190, 195, 196,-207, 215, 
 218, 219, 222, 224, 228, 229, 
 230, 231, 234, 246, 248, 262, 
 266, 268, 280, 281, 282, 284, 
 286, 287, 289, 359, 368, 374, 
 878, 386, 891, 393, 394, 396, 
 399, 400, 456, 463, 464, 465, 
 478, 480, 485, 495, 496, 497, 
 500, 504, 511, 518, 520, 522, 
 526, 540, 544, 550, 553, 555, 
 563, 565, 566, 567, 568, 569, 
 570, 571, 572, 573, 586, 594, 
 606, 607, 624, 641, 642, 644, 
 646, 652, 667, 668, 673, 735 
 
 Dalman, J. W. we «= 44, 65, 244 
 Dalry mple, ¢ er } Elphinstone fs pee Ghe 
 Dana, J. D. 44, 60, 159, 175, 179, 184, 185, 
 189, 193, 195, 205, 207, 218, 
 221, 226, 227, 236, 237, 238, 
 240, 248, 251, 264, 266, 269, 
 273, 277, 278, 280, 282, 283, 
 254 204,20, 558, 569, 583 
 Daniels, J. : nae eee G02, 
 Darwin, Charles . 202, 553, 698 
 Daudin, F. M. Seo ta AY 
 David, T. W. Edgeworth 74, 171, 308, 309, 360, 
 
 Davidson, T. 
 
 Davies, W. 
 
 Dawson, J. eliani | 
 
 362, 459, 479, 542, 563, 564, 
 565, 566, 567, 568, 574, 578, 
 596, 598, 601, 618, 637, 733 
 
 .. xvi. 64, 66, 67, 68, 226, 227, 
 
 229, 230, 233, 235, 236, 242- 
 248, 253- 264, 409, 442, 4.44, 
 te 650, 661 
 
 36, 43, 49, 132, 
 
 191, 192, 196 
 
 Debay, a aie 557 
 De Boilev evil We ae ToL 
 Defrance, J. L. M.... "4d, 67, 92, 94, 
 
 183, 254, 287, 484, 
 Deuton, W. Wie 617, 639 
 Desgrand, J. V.S.... w. «= 424 
 Deshayes, G. P. 2, 635, 641, 693, 694: 
 Deslonchamps, E. ... eG 44.2, 443 
 Dixon, W. A. aE : 330, 358 
 Draparnaud, J. P. R. ae saa .. 644 
 Duclos, P. L. a 695 
 Dutton, C. E, 590 
 
 EDELFELT, Eric 
 
 Edkins, FE. R. 
 Edwar ds 
 Haime 
 
 Eichwald, E. von. .. 
 
 Embly, J. T. 
 Etheridge, Robert . 
 
 (Milne- Edwar ds) 
 
 204, 226, 230, 232, 
 275, 277, 690, 697 
 . 407, 464, 502 
 and 
 43, 44, 50, 2, 53, 5D, 
 58, 60, 61, 68, 201, 691 
 43, 56, 225, 466, 477 
 act Moe eke) 
 xvi., 19, 72, 
 "83, 84, 92, 98, 94, 129, 180, 
 141, 151, 158, 159, 161, 184, 
 193, 214, 215, 217, 224, 227- 
 231, 234, 245, 246, 248, 255, 
 258, 259, 262, 266, 267, 268, 
 279-282, 284, 286, 287, 289, 
 392, 393, 395, 396, 399, 406, 
 
 
 
 Page: 
 
 Etheridge, Robert—continued. 
 
 Ettingshausen, C. von 
 
 409-412, 440, 455, 456, 458, 
 459, 460, 463, 464, 465, 469, 
 471, 474-480, 484, 485, 492, 
 494, 495, 496, 500, 504, 531, 
 544, 554, 555, 563, 565-571 
 311, 315, 351, 368, 
 557, 580, 581, 596 
 
 Fasricivs, J. C. wo = AAD 
 Falconer, John _ 825, 407, 429, 
 446, 511, 590 
 Feilding, W. a : 399 
 Feistmantel, Ottokar - fica eas 
 
 Fichtel and Moll 
 Fischer, Paul 
 
 Fitzinger, L. J. 
 Fitzwalters, G. 
 Fleming, John 
 
 Fletcher, Joseph 
 Foord, A. H 
 Forbes, Edward 
 
 Forsyth, William . 
 Francis, W.... 
 
 Fritsch, K. von 
 Frost, R. W. 
 Fryar, William 
 Fuess, R. : 
 
 Gass, W. 
 
 Geinitz, H. B. 
 Geoffroy, — 
 Germar, E. F. 
 Gmelin. sc 
 Goeppert, H. R. 
 Goftage, — .. 
 Goldfuss, G. A. 
 
 Goldie, Andrew 
 Gordon, W. P. 
 Gould, C. 
 Grand ’Eury, E. 
 Gray, J. E.... 
 
 Gregory, A. C. 
 
 Gregory, F. T. 
 Grey, Robert, 
 
 Grey, Mrs. Robert... 
 
 Griesbach, C. L. 
 Griffiths, G. N. 
 Griffiths, G. 8. 
 Guembel, G. 
 Gulland, James 
 Gunther, Albert 
 
 63, 64, 69, 201, 223, 461, 484 
 
 568, 572, 601, 606, 639, 739 
 
 Pl 137, 140, ‘141, 179, 189, 
 190, 193- 197, 313, 315, 316, 
 B17, 828, 352, 354, 856, 357, 
 2, 363, 367-371, 373-378, 
 ae 381, 384, 386, 557, 558 
 a5 409, 435 
 
 “Ady, 67, 68, 244, 
 
 278, 288, 443, 560 
 
 ... 648 
 
 ‘ 514 
 
 "130, 137, 141, 
 
 182, 235, 655, 694 
 
 A¥ 331 
 
 43, 48, 53-56, 65 
 
 . 409, 470, 483, 
 
 571, 691, 697 
 
 Be PAs 
 
 xv. 
 
 Oa 
 
 a 651, 680 
 
 138, 189, 197, 341 
 Ou 
 
 +  asepaaara 
 488 
 
 . 265, 368, 493 
 664, 681 
 
 140, 141, 178, 188 
 
 . 476 
 
 "192, 311, 315, 367,379 
 
 '" A0T, 469, 473, 488, 484, 494 
 
 43, 44, 48, 49, 50, 58, 59, 61, 
 
 687 
 
 a 390, 512 
 
 633, 634, 640, 674, 676 
 43, 49 
 
 484, 635, 645, 646, 648, 
 649, 674, 692, 695, 698 
 
 Ac fo a0 <o ea Les 
 4,34, 60, 72, 73, 74, 300,. 
 
 301, 302, 304, 307, 327, 333, 
 341, 347, 350, 369, 370, 373, 
 382, 389, 406, 407, 445, 446, 
 447, 454, 456, 462, 466, 473, 
 475, 476, 483, 501, 521, 566, 
 
 521 
 
 407 
 
 289 
 
 567, 568 
 
 432, 631 
 
 Ro abe 
 cs tae ee 
 345 
 
 646 
 
HAAN, W. de 
 Hacket, T. R. 
 Hague, Arnold 
 Hall, James 
 
 Hall, Richard 
 
 Hall and Whitfield _ 
 oe Albany... 
 
 Hanley, 8. ... 
 Hann, William 
 Harkness, R. 
 Hartmann, C. H. 
 Haswell, W. A. 
 Hauer, Carl yon 
 Haughton, S. 
 Heaviside, E. 
 Hector, James 
 Hedley, C. .. 
 Heer, O. 
 Henderson, - B. 
 
 Hester, R. ... 
 Hizhley, Perey 
 DS eb Se ek 
 Hincks, T 3h 
 Hinde, G. J. 
 Hinds, R. B. 
 
 Hochstetter, F. von 
 
 Hodgkinson, W. O. 
 Holmes, A. E. 
 Holzapfel, — 
 Hood, J. H.. 
 
 Hope, F.W. 
 Hudleston, W. H. 
 
 Hughes, H. ... 
 
 ... 891, 463, 501, 531, 536,539 
 
 INDEX TO PERSONS. 
 
 Page. 
 
 ses wes | 204 
 
 72 
 
 627 
 
 "43, 53, ‘6B, 59, 62, 64, 
 
 “65, 244, 247, 253, 265, 270 
 
 276, 290, 453, 482 
 An eave 
 
 272, 273 
 
 298 
 
 635, 640, 695 
 
 272, 273, 
 
 ane 652 
 
 379, 381, 666, 672, 682 
 221 
 
 491 
 
 197 
 
 388 
 
 361, 488, 508, 509, 510 
 A 643 
 
 wat 316, 317 
 
 322, 323, 404, 407, 414, 
 417, 462, 465, 469, 478, 
 494, 502, 512, 516, 739 
 153, 234 
 
 Ree XV1. 
 
 664- 668, 672, 677 
 
 ote 904 
 
 xi., 59, 63, 209, 436, 438 
 ith 695 
 
 484, 
 
 Xiv., d21 
 
 138, 192 
 
 293 
 
 668 
 
 2 388 
 
 “409, 451, 466, 467, 473, 474, 
 478, 479, 481, 484-487, 493 
 667, 668, "673, 674, 677 
 
 Hughes, Joseph came ORG 
 Hull, Robert 157, 233, 234, 
 
 257, 270, 273 
 Humboldt, A. yon... = 734 
 Biarstes Ll. wwe . 653, 656, 657 
 Hutton, F. W. -.608, 619, 703, 
 
 706, 732, 734 
 Huxley, T. ... 634, 636, 687, 650, 669 
 Isaac, F. N. ...065, 667, 668, 669, 677, 683 
 JARDINE, John... 20 ae 10608 
 Johnston, G. x oe 441 
 Johnston, R. M. 2, 317, 361 
 
 Jones, T. Rupert 
 
 Judd, J. W. 
 Jukes, J. Beete 
 
 Karsten, D. L. G. 
 Kaufmann, J. M. 
 Keene, W. ... 
 Kennedy, E. B. 
 Kent, W. Saville 
 Keyserling, A. yon 
 Kidston, Robert 
 
 xvi., 130, 137, 141, 181, 
 214, 353, 354, 363, 387 
 Pe oe fOb 
 
 : 195, 615, 617 
 
 502 
 
 222 
 
 195 
 
 541 
 
 a OLe 
 
 f 460, 461 
 
 oe Xvi., 189, 190; 
 193, 194, 196, 315, 369, 
 370, 374, 381, (382, 383 
 
 
 
 
 
 King, G. 
 King, W. 
 
 iKilemad «Esa. 
 Kléden, K. F. 
 Kock, F. de 
 Konig, C. 
 
 Koninck, iG de) a 
 
 Krauss, C. F. F. 
 Krefft, Gerard 
 
 A Gina SIS mane 
 
 745 
 
 Page. 
 ee. Aeche Mey ke) 
 158, 159, 183, 220, 
 
 225, 242, 246, 258, 260, 
 261, 275, 281, 453, 456 
 447, 478, 479, 570, 641 
 e466 
 sane LOB 
 
 83, 159, 182, 232, 505 
 43, 44, 48, 52, 53, BG: 60, 
 61, 64, 68, 69, 73, 84, 92. 93, 
 94, 130, 137, 141, 157, 158, 
 159, 181, 182, 185, 186, 209, 
 215, 217-222, 224, 225, 226, 
 228-234, 236-240, 242-246, 
 248, 250, 251, 252, 254, 255, 
 
 258, 260, 262, 263, 266-272, 
 
 274-277, 279, 281, 282, 283, 
 285-288, 290, 291, 293-296 
 198, 567 
 
 .. 505, 633, 634, 
 
 646, 658, 663, 681 
 
 323, 353, 354, 363, 381 
 
 Lamanrcke, J. P. B.A.de M. 43, 48, 50, 52, 274, 
 
 Landers, W. 
 Latreille, P. A. 
 Laurenti, J. N. 
 Leach, W. 2 
 Learmouth, F. 
 Lehon, H. 
 Leibius, A. ... 
 Leichhardt, L. 
 Leigh, W. 
 
 Lendenfeld, R. yon. 
 
 Lesquereux, L. 
 Lesson, R. P. 
 Léveillé, C... 
 
 Leymerie, A. 
 
 Lindley and Hutton 
 
 Lindon, E. B. 
 Lindstrém, E. 
 Link, J. W.... 
 Linneus, K. 
 
 Linthwaite, F. 
 Lister, M. 
 Liversidge, A.... 
 
 Livesey, H. G. 
 
 Lonsdale, W. 
 
 Loriol, P. de 
 Lycett, J. 
 Lydekker, R. 
 
 Lyell, Charles 
 Lymburner, A. 
 
 645, 654, 655, 656, 658, 695 
 
 275, 435, 444, 453, 466, 468, 
 469, 473, 474, 478, 481, 482, 
 485, 486, 565, 568, 570, 572, 
 635, 642, 643, 644, 693, 694 
 eae Sa 407 
 
 639 
 
 652 
 
 655 
 427 
 
 209 
 600, 601 
 35, 59, 604, 668 
 
 .. 210 
 
 619 
 
 peer i08 
 
 606, 632, 641, 692 
 
 92, 94, 243, 245, 
 288, 290, 291, 499 
 
 E es 7, 
 
 ” 192, 318, 352, 
 
 354, 363, 379, 380 
 
 . 808 
 
 43, 51 
 
 =. 278,566 
 “44, 65, 381, 356, 364, 
 440, 445, 450, 453, 465, 468, 
 475, 481, 483, 561, 572, 640, 
 
 308 
 oe 491 
 
 79, 252, 261, 262, 
 “462, 463, 4.64, 491, 
 498, 501, 502, 505 
 ; 609 
 
 "43, 58, 62, 83, 92, 93, 94, 151, 
 
 159, 181, 202 , 203, 204, 207, 
 
 217, 218, 220, 221, 222, 223 
 
 a: 440, 473 
 
 470, 471, 477, 484, 568 
 305, 647, 648, 649, 
 651, 658, 661-667, 
 672-678, 680, 681 
 
 = 879, 735 
 
 aia 497, 508 
 
746 INDEX TO PERSONS. 
 
 Page. 
 
 McCiELLAND, J. 352, 356, 362, 373 
 McCoy, F. ... - EAT 3, 
 xvi., 60, 62, 63, 66, 84, 92- 95, 
 
 116, 128- 131, 135, 137, 140, 
 
 141, 157, 159, 175, 177-180, 
 
 182-186, 190, 191, 194, 195, 
 
 196, 198, 201, 213, 214, 217, 
 
 218, 219, 221, 225, 229, 234- 
 
 237, 239, 243, 245, 246, 250, 
 
 255, 262, 263, 265, 266, 268, 
 
 272-275, 277, 278, 280-286, 
 
 291, 296, 311, 312, 316, 317, 
 
 323, 351, 352, 354, 356, 360, 
 
 366, 368, 371-374, 394, 400, 
 
 406, 407, 411, 412, 413, 440, 
 
 452, 463, 464, 470, 489, 490, 
 
 491, 494, 496, 497, 498, 505, 
 
 507, 508, 510, 520, 560, 694: 
 
 MeDonald, H.C. ... pane mee) 
 Macdonald-Cameron, J. 599, 601 
 Macfgillivray, John 450 541, 689 
 Macgregor, William a oe 684, 686, 
 687, 690, 712, 714, 
 719, 721, 735, 736 
 157, 191, 194, 
 226, 229, 239, 262, 
 279, 288, 290, 291 
 
 Mackay, Herbert 
 
 Mackinnon, W. ... cA 321, 407, 5C6 
 Macleay, William ... 690, 692, 693, 694, 698 
 McLellan, J. ve gen te Y/ 
 Macmillan, A. C. : . 407, 501, 531 
 Macpherson, A. ... sa a oe OLS 
 Madden, A. J. es Aa ae OA 
 Maitland, A. Gibb .. ix., xiv., 7, 39, 
 
 134, 143, 146, 157, 168, 72s 
 417, 521, 524, 526, 528, 533, 
 546, 554, 556, 583, 587, 592, 
 593, 616, 622, 630, 684, 705, 
 TO MAG Lo aoa Onnaleds 
 718, 722, 724,725, 728, 732 
 Mantell, G. A. . 406, 411, AGA, 465, 493 
 Mantell and Sowerby Sete = 468 
 Mar, Robert 322, “423, 424, 425, 
 
 428, 429, 430, 627, 631 
 March, — ... eee ae Grae LOA: 
 Martin, K. ‘ 88, 92, 93, 94, 130, 
 137, 141, 159, 182 , 18a; 
 226, 227, 230, 235- 238, 
 244, 254, 255, 569, 691 
 
 Martyn, W. C. me ; pe OAG 
 Massalongo, AS be P. : a5. DDO 
 Meek, 1 ‘B. 212, 223, "924, 264, 265, 
 
 274, 275, 276, 278, 279, 
 819, 446, 448 452, 465, 
 470, 475, 476, 486, 561 
 
 Meek and Worthen ; sa 274, 275 
 Megerle, — (vide “ Mithlfeldt) a teat a OE 
 Ménard de la Pare F.J.B.  ... 478, 479, 570 
 Merran, B. ... “a ee OO 
 Meston; A. ... ar a ae anc lee ateiy 
 Meyer, 'H. von A Bes a: ein 204s 
 Miklouho-Maclay, A. de 690, 695 
 Miller, 8. A. ir . 98, 180, 207, 
 
 208, 209, 291, 439 
 Mitchell, Thomas L. 304, 668, 673, 674, 677 
 Moffat, John, and Co. ae LZ 
 Mojsisovies, E. von xis ves we 402 
 Montfort, D.de_... tip 289, 484 
 Moor, J. Hugh ... .., 407, 417, 506 
 
 Page. 
 . xiv., 391, 394, 396, 409-413, 
 "434, ‘435, 7436, 438-453, 455, 
 457-460, 462, 466- 4vl, 473- 
 478, 480, 481, 483-488, 499, 
 500, 505, 512, 554, 560, 565, 
 564, 567, 568, 571, 573, 697 
 Morelet, A.... Se ane w. 648 
 Morris, John ce 5 72, 84, 92, 94, 157, 
 159, 178, 181-186, 189, 190, 
 193, 194, 193, 217, 225, 226, 
 228, 230-233, 237-241, 248- 
 252, 254, 263, 266-269, 271, 
 275, 277, 218; 2825 283, 284, 
 286, 287, 291, 294, 295, 311, 
 312, 314, 316, 317, 351, 352, 
 354, 356, 357, 360, 362, 368, 
 369, 370, 380, 381, 382, 740 
 Morris and Roberts Aes mo 2k) 
 Morris and Sharpe... +e 33 ter aoe 
 Morrisby, Rowland : 407, 474, 483, 487 
 Morisset, A. L. Asc 157, 208, 232, 233, 235, 
 241, 248, 252, 254, 264 
 
 Moore, Charles 
 
 Mosely, H. N. = aOol 
 Mosman, H. aoe 4706, 725 
 Moss, R a es ae a5 A y 
 Mueller, Ferd. von a w= O88 
 Mueller, O. F. 445, 467, 692 
 Mihlfeldt, Mergele ¥ yon . 812, 319, 641 
 Mulligan, James We 125, 539 
 
 Miinster, Georg von 
 Murchison, R. I. nae sae 
 Murphy, F.R. ... aoe ae ve 
 Murray, Peter... in sh ave W40) 
 Murray, Reginald A. F. St 45, 575 
 Musson, C. T. a .. 188, 296, 643 
 
 eh 
 ao = 868 
 
 
 
 Naruorst, A.G. ... sae 298, 372 
 Newbery, J. Cosmo ae sa oe aoe 
 Newberry and Worthen... §y) M3 ZG 
 Newton, R. B. Se ee ut peas eS Qe 
 Nicholson, C. 6738, 678 
 Nicholson, F. 666, 668 
 Nicholson, H. A. XV kV 
 
 43, 44, 48, 49, “50, él, 53, 54, 
 56, 57, 58, 61, 62, 63, 64, 
 137, 151, 159, 180, 202, 203, 
 204, 205, 206, 289, 298, 299 
 
 Nilsson, 8. ... ce 469 
 Oaa, H. K,. Ae e: aye aT 
 Ogilby, J. Douglas... on MP «se BSB08 
 Ogilby, W. . a Pre 
 Oldham end Feistmantel . 364 
 
 Oldham and Morris ‘, 872- 375, SY Ee 
 392, 525, 554, 557 
 Olliff, A. Sydney = ’ 858,368, 387 
 Oppel, Alba x ee Gua 
 Orbigny, Alcide@ ... 72, 84, 92, 94, 159, 183, 
 202, 228, 232, 233, 284, 240, 
 247, 248, 256, 2577, 291, 409, 
 435, 436, 442, 463, 464, 465, 
 471, 472, 486, 487, 491, 492, 
 493, 495, 497, 499, 561, 566, 
 569, 571, 574, 696, 697, 698 
 Hh ; xiv., 396, 
 412, 437, 505, 507- 510, 606, 
 609, 683, 634, 635, 646, 651, 
 658, 662-669, 672-681, 683 
 
 Owen, Richard 
 
INDEX TO PERSONS. 747 
 
 Page. 
 PauMER, F.... =r Se 624, 631 
 Parker and Jones... * .., » 4386 
 Parkinson, J. a ht 462, 494, 496, 567 
 Peale, A. C, ie ae ieee ALD 
 
 Pears, P. W. 135, 196, 197, 215, 
 245, 285, 291, 407 
 
 635, 645 
 
 : 445, 695 
 
 | 44, 67, 68, 72, 84, 92, 93, 
 “94, 130, 133, 137, 138, 141, 
 151, 159, 177, 181, 182, 183, 
 185, 224, 229, 233, 236, 242, 
 244, 245, 246, 274, 285, 286, 
 872, 409, 410, 411, 440, 447, 
 473, oth 488, , 489, 491, 492 
 
 Pfeiffer, L. ... 
 Philippi, R.A. 
 Phillips, John 
 
 Phillipsson, L. . 888, 468, 482 
 Pichl, ~- ee rs 217, 219 
 Pictet, ine mrs) ime ee en 40 7 
 Pictet and Campiche 445, 567 
 Pictet and Roux ... sar oe 453 
 Pilsbry, H. A. ae voce eine w= 645 
 Pittman, E. F. an3 ne scar more 
 Plews, H. T, ~ ch aie Noohy Whee 
 Po lisGra kee vee a re ay 475 
 Portlock, J. HE. A “914, 224, 
 Presi J: S:... 323, 354, 363, 377 
 QUENSTEDT, F. A. ... see se FOO0 
 RAFINESQUE, — = 200, 245 
 Ramm, T. W. 397, 407, 489, 491 
 Ramsay, E. P. 505, 608, 681 
 
 Rands, William H.... ix. ‘xiv, 16, 17, 18 
 20, 23, 32, 33, 35, 42, 50, 
 74, 83, 84, 85, 87, 89, 90, 
 97, 98, 99, 101, 102, 105- 
 109, 135, 140, 143, 158, 193, 
 201, 219, 234, 236, 240, 243, 
 244, 245, 252, 255, 264, 266, 
 273, 276, 279, 287, 291, 296, 
 800, 801, 802, 304, 305, 307, 
 810, 311, 315-322, 324, 328, 
 350, 357, 454, 518, 528, 543, 
 546, 558, 562-566, 571, 574, 
 582, 598, 595, 596, 610, 611, 
 4701, 706, 721, 735, 736, 737 
 
 Raspail, B. ... i a 496 
 Ratte, Felix 283, 284, 499, 500 
 Rattray, AS Fe ad ris wu Ol4 
 Raynal, F. M. 58 at 250 ... 649 
 Recluz, E. ... Sar .. 486 
 Reeve, L. .. .. 641, 643, 645, 646, 694, 695 
 Reuss, H. A. aa ane OOO. 
 Rickard, T. A. me age oa OO 
 _ Ridley, Stuart “D0 50¢ a San Ve 
 Ringrose, RK. C. _... 3dr 366, 369 
 Robertson, J. R. M. me 804 
 
 72, "212, 213, 295, 
 298, 389, 447, 465 
 Roeminger, C. se 43, 51, 52, 53, 54 
 Rogers-Harrison, — ae 140 
 Rosenbusch, H. 702, 703, 704, 708, 
 713, 714, vate 720 
 
 Roemer, Ferd. yon 
 
 Royle, J. F. . 852, 354, 356, 366, 370, 418 
 pee and Strauss 387 
 Rutley, F . 714, 715, 731, 732,733, 735 
 Ryan, D. P. 407, 504 
 
 Ryckholt, P, de : 1, meee, os 2hB76 
 
 - Smith, James 
 
 
 
 Page, 
 649, 666, 668, 672 
 
 St. JEAN, 8. exit 
 
 Salter, J. W. 297 
 
 Samwell, W. 28, 30, 454, 554, 561, 563, 573 
 Sandberger, y; * i 67, 295 
 
 Sandberger, G. and F. a i 69 
 
 Sanders, — ... ost acy | ekeuk 
 
 311, "317, 356, 375, 
 
 876, 386, 740, 741 
 
 315, 319, 379, 380 
 
 189, 198, 198, 316, 317, 
 319, 352, 356, 368, 372, 375, 
 376, 379, 380, 386, 392, 557 
 Schlotheim, F. E. von 44, 64, 68, 140, 
 141, 178, 189, 246, 
 
 461, 476, 488, 561 
 
 Saporta, G. de 
 
 Schenk, A. ... 
 Schimper, W. P 
 
 Schmidt, Oscar... aS an .. 4388 
 Schneider, — 4.87, 632, 633, 652 
 Schnur, J. ... an te ne . 4A, 65 
 Scopoli, J. A. ate sf 00 1646 
 Scott, Walter nie Soo nee OG 
 Scoullar, Gavin ,., ae ae Jeu SOUS) 
 Sefton, R. ... fe te se 407 
 Sellheim, Pp. FB. ay. a . 407, 489, 713 
 ‘Selwyn, A. R. OC. ... 800 . 560 
 Sexton, R. ... a . 197, 407, 495 
 Sharpe, Daniel 263, 493 
 
 Sharwood, S. 405, 407, 462, 465, 
 
 ‘469, 470, 491, 498, 502 
 
 Shaw, G. ... .. 633, 634, 648, 655, 672, 681 
 Sheehy, — ... sn ate Pe OUS: 
 Simmonds, J. H. 347, 387, 388, 441 
 Skene, J. ... i BR 
 
 Smith, Edgar A. ba He , 486, 640, 641, 642, 644 
 x Xill, XlV+, XVI, oo, 
 89, 90, 92, 95, 138, 139, 143, 
 1517, 158, 171, 189, 192, 194, 
 196, 202, 206, 209, 210, 212, 
 215, 216, 218, 219, 224, 225, 
 229, 231, 234, 236, 239, 243, 
 244, 245, 248, 252, 254, 255, 
 256, 260, 262, 263, 268, 269, 
 285, 286, 287, 290, 295, 296, 
 297, 299, 308, 343, 355, 364, 
 370, 376, 377, 382, 383, 386, 
 407, 447, 449, 491, 492, 494, 
 598, 601, 640, 645, 646, 683 
 
 Smith,— ... nes 352, 371 
 Smyth, R. Brough ... ci : 622, 623 
 Sollas, W. J. se ate ee ww. «= 48 
 Sorby, tags pace ORAL 
 Souttar, W. . 865, 367, 369, 370, 374, 381 
 Sowerby, George = 87, 92, 94, 157, 
 
 159, 177, 183, 248 
 Sowerby, George B. 83, 92, 93, 
 
 94, 157, 158, 159, 182, 
 212, 228, 231, 232, 238, 
 240, 241, 249, 250, 573 
 
 44, 60, 64, 67, 72, 93, 
 
 94, 182, 183, 227, 233, 247, 
 255, 256, 264, 285, 291, 293, 
 295, 411, 412, 444, 445, 446, 
 462, 471, 493, 561, 695, 696 
 Sowerby, James de Carle 66, 88, 92, 93, 94, 
 182, 183, 185, 226, 230, 
 
 243, 278, 282, 283, 286, 
 
 287, 461, 561, 565, 696 
 
 Spencer, A.... aE ase | ay) 
 Spengler, L.... bas ial » — 482 
 Staiger, Karl T. .., . 175, 392, 630 
 
 Sowerby, James 
 
748 
 
 Stephens, W. T. 
 
 Sternberg, — von ... 
 
 Stirling, James 
 Stokes, Henry G. 
 Stoliczka, F 
 
 Storr, G. C.. 
 Strattera 
 Strzelecki, P. E. de 
 Stutchbury, Samuel 
 
 Suckow, G. A. 
 Swainson, W. 
 Sweet, George 
 
 Sykes, William H.... 
 
 Sythers, T 
 
 BONE Se ae 
 Tate, Ralph 
 
 Taylor, Norman 
 
 Teall, J. J. Harris ... 
 
 INDEX TO PERSONS. 
 
 Page. 
 
 .. Xvil., 875, 697 
 
 _ 129,140, 141, 
 
 179, 188, 196, 311, 316, 
 352, 353, 356, 370, 383 
 oe Gat 
 
 .. 822, 59h, 739 
 
 282, 320, 447, 
 
 “448, 460, 461, 465, 456, 467, 
 
 476, 478, 481, 482, wee 493, 
 494, 496, 566, 569, 570, 572 
 : ” 70 
 ter WW aGTSt) 
 217, aaes 283, 683 
 
 ’ Ty Vier Ons, aces 
 pit 617, 618, 672, 739 
 Nice 188 
 ; 476, 655 
 69, 239, 282, 316, 
 
 "368, 369, 377, 378, 399, 407, 
 
 44.2, 443, 446, 451, 456-460, 
 462, 466, 472, 479, 486, 495, 
 496, 500, 501, 504, 509, 533, 
 559, 560, 562, 568, 564, 565, 
 566, 568, 570, 571, 572, 574 
 
 te e : 601 
 
 xiii. 
 
 # . 299, 408, 409 
 
 xvi, 353, 354, 363, 389, 
 
 394, 403, 406, 407, 410-413, 
 444, 446, 448, 451, 452, 454. 
 459, 467, 469, 472, 478, 475, 
 479, 483, 484, 485, 488, 490, 
 491, 546, 563, 564, 571, 573, 
 574, 609, 618, 623, 644, 740 
 ..176, 391, = 
 
 406, 440, 493, 499, 520, 52 
 
 528, 581, 536, 539, 554, 539 
 702, 720, 729, 730, 734: 
 
 Temminck, (Oredig hon 680 
 Thompson, Basil H. coe é 687 
 Thompson, J. Malbon-_... Soh ae) ESO 
 Thompson, William 739 
 Tooth, W. F., Junr. 673 
 Trautschold, H. : 559 
 Troost, G. 211 
 Tryon, H. 5, ae 
 Turner, — 664, 665, 668 
 
 Uxricn, E. O. 
 Unger, F. F. 
 
 VERBEEK, R. D. M. 
 Verneuil, KE. de 
 Viellot, L. P. 
 
 Vine, G. R. 
 
 Vis, C. W. de 
 
 43, 55, 223, 224 
 ;. 196, 198, 317 
 
 a oor 
 289, 291 
 661 
 
 223 
 
 xvi:, 90, 
 
 "92, 115, 157, 188,191, 194, 
 
 199, 200, 201, 207, 208, 210, 
 211, 213, 216, 223, 226, 227, 
 228, 230, 233, 235, 238, 239, 
 245, 246, 256, 262, 269-274, 
 
 
 
 
 
 Page. 
 Vis, C. W. de—continued. 
 279, 286, 288-297, 299, 407, 
 456, 489, 499, 503, 508, 510, 
 612, 633, 634, 635, 639, 646, 
 
 647, 649, 651- 658, 661- 667, 
 669-673, 675, 679-683, 740 
 Visiani, R. de oe Pin st, 
 Vogan, A. J. a ie 371, 378, 626, 695 
 Violtz, Pe Eicre ae we 5a Oe 
 Vosmaer, A. fae woe wae jue 438 
 
 Waacen, W. . 68, 206, 221, 
 235-239, 242, 246, 
 258, 254, 256, 257, 
 263, 453, 499, 696 
 
 217, 219 
 
 Waagen and Pichl... fy 
 56, 58, 202, 206 
 
 Waagen and Wentzel 
 
 Wachsmuth, Charles aa Bo acl le%s 
 Wadsworth, M. E. oe we Spies 
 Wahlenberg, G. ... ae ioe ten PAG 
 Walker and Jacob ... a 4p 409, 436 
 Walcott, C. D. roe se ee Joe wan) 
 Wallace, Alfred ia aes mae va SOUS) 
 ‘Walsh, W m. 4 sce my 318, 380 
 Waterhouse, G. R. “ai a6 eos 
 Webb, — Boe ESE co 
 Weed, Walter H... te sas cory ES) 
 White, CAs pee ae See pets} 
 White, W. T. fe ate Pr eo oo 
 Whitelegge, T. ae ies ae XVI, LOD 220 
 Whitfield, iv fi . 272, 273, 482 
 Wilkinson, Charles S. 141, 142, 
 
 170, 359, 360, 372, 487, 514, 
 542, 553, 578, 598, 601, 608, 
 609, 614, 631, 685, 686, 690, 
 
 694, pdf 723, 724, 728, 735 
 Winwood, H. H. ‘ : xvi., 481 
 Wood, W. ves uae xiii. 
 Woods, Julian HB. Tenison .. see wees 
 
 XVii., 71, 138- 141, 177; 178, 
 
 179, 188- iieht, 196, 197, 198, 
 
 293-295, 301, 311-316, 318, 
 
 319, 322, 342, 344, 351-356, 
 
 359, 362-365, 367, 369, 370, 
 
 371, 373-378, 380-386, 397, 
 
 409-413, 446, 453, 454, 457, 
 
 466, 467, 470, 471, 477, 488, 
 
 489, 492, 498, 499, 501, 502, 
 
 527, 543, 544, 553, 555, 568, 
 
 572, 614, 621, 685, 686, 690, 
 
 691, 692, 694, 695, 697, 739 
 
 Woodward, A. Smith 136, 296, 360, 407, 
 412, 503, 504, 633, 646, 647, 649 
 
 Woodward, Henry Xvi., 383, 399, 412, 
 441, 493, 697 
 
 Worthen, A. H. 212, 263, 274, 275, 296 
 
 Youne, John 203, 223 
 Young, John co et 
 Zrano, A. de te 318, 380 
 Zirkel, Ferd. .. 702,730, 782 
 Zittel, Karl A. 224, 438, 461, 465 
 
INDEX TO PLACES. 
 
 
 
 )>—_—_———- 
 
 Page. Page. 
 ABERDARE ... . 341, 351, 368 Beverley Islands... 500 a ton (oll 
 Adavale “at a ae 427,513 Bindi, Victoria .- ... nas ais as 45 
 Agate Creek ae oh Ss 522, 523 * Birkhead Creek ... 366 ae peDLO 
 Ageston.... wey 33 seit 3 328 Birnam Range se Si OOO. 
 Albany Pass sag ets Sf 542, 616 Blackall te 405, 411, 414, 416 
 Alberton ... me oo. GyAs! 424, 471, 492, 515 
 Albert River aie 324, 850, 548, 544 Blackfellows’ Creek, near Too- 
 Alice Downs ae , oo © 2 woomba -... : i 338, 341 
 Alice River ... ao re nw sao aa Blackfellows’ Diggings 92,178, 219, 222 
 Allingham’s Creek ... $e a) OSS. Black Snake MESA PK SOs00 7. 
 Allora ee ae eh at to BO Blair Athole ae 167, 170 
 Alpha a eS ss sah er ROLG Blenheim ... oc eee pL 
 Ambatalla Creek ... soo. cele Bloomfield River, near Cooktown... er 10 
 Amby River . 390, 410, 480, 481, 511, 512 Bloomsbury... ee Loo 
 Amelia Creek oes = OG Blue Mountains, N.S. Wales 176, 528, 554, 614 
 
 America, North 415, 418, 428, 431, 
 
 564, 590, 608, 627 
 
 America, South .... see . 608 
 Angellalla Creek ... e ant rob, fabs 
 Angellalla Range ... aa 512, 514 
 Angy Springs nf ai Sid, kept 
 Annan River, near Cooktown 4c. 10, § 529 
 Apis Creek . F se 178, 222 
 
 Aramac “405, 411, 416, 425, 447, a 
 
 465, 469, 470, 480, 482, 491, 
 492, 494, 495, 498, 502, 515 
 
 Argentine : ste OX, 45, 129 
 Arthur’s Creek "85, 48, 50, 54, 61, 64 
 Athelstone Range, Rockhampton... 90, 91, 93, 
 
 262, 263, 299 
 Augathella ... : tts 426, 515 
 Avon Downs en sa ia .. 419 
 Avon River, Victoria ber ‘or me we 142 
 Ayrshire Downs eas 402, 421 
 Baconts Marsu, Victoria ane OLS 
 Back Creek ... & 500 ... 416, 423, 424 
 Ballandean ... a ae Be £ xii. 
 Balonne River aes rE .. 614 
 
 Banana Creek 143, 15! 575 , 178, 226, 229, 
 232, 233, 239, 262, 266, 
 
 277, 279, 288, 290, 291 
 
 . 411, 414, 416, 423, 491, 495 
 
 405, 411, 462, 467, 
 
 513, 515, 516, 631 
 
 Barkly Tableland ... a si 894, 397, 418 
 
 Barrier Range, N. S. Wales ae fon gp SOLA: 
 
 Barron River . 122, 586, 588 
 
 Barcaldine... 
 Barcoo River 
 
 Basalt Wall tee 594, 738 
 Batavia River soa ot 
 Battle Camp , 580, "532, 533, 5385, 554, 555 
 Beaconsfield : : 178, 201 
 Beaudesert ... a soo BB) Be, EID 
 Bee Creek ... eae a a 167, 168, 169 
 Beenleigh ... ey ae xi., 824 
 
 Bellenden-Ker Range 1, 122, 592 
 Belyando River ... re 515, 516 
 Berserker Range, Rockhampton Aa 91, 683 
 Betts’ Creek ae bor ... 518, 554, 659 
 
 
 
 
 
 Blythesdale... . 410, 456, 459, 477, 486, 512 
 Bogantungan suc se . 188, 188, 189, 
 156, NGYZ 198, 296 
 
 Bogie River... aap jae 50 Fac 31 
 Bollon ant ¥n sac ay 429 
 Boolboonda... ‘ 17, 18, 87 
 Boyne River ae am ee Ree vii. 
 Boulia 485 aay Aes abe 556, 631 
 Bowen Downs Br as 411, 422 
 Bowen River 56 ee Isp ss KV OU: 
 70, 96, 97, 143, 144, 150, 
 
 158, 159, 161, 167, 168, 177, 
 
 178, 190, 194, 195, 198, 204, 
 
 205, 208, 218, 222, 223, 226, 
 
 228, 229, 230, 232, 239, 241, 
 
 247, 252, 254, 260, 262, 266, 
 
 267, 271, 275, 277, 280, 281, 
 
 282, 284, 294, 295, 520, 525 
 
 Bowra Creek Sse ape 860 sop AOS 
 Boyne River Bas ee sor =. 30,.59 
 Bradley’s Creek... eee dat sua tall 
 Braeside shea fia G 343, 345 
 Brazil vas Ras as as .. 407 
 Breadalbane 380 .. 482 
 Bremer River Vile; 886, 344, 353, 388, 389 
 Bribie Island se OLS 
 Brinsop ena ane ane oe seo, ULE 
 Brisbane... te, Be Tis, Xils, Oss, 
 
 821, 341, 352, 369 
 Vil., Vill., 5, 337, 841, 369 
 95, 178, 222, 300 
 
 Brisbane River 
 Broad Sound 
 
 Broken Hill, N.S. Wales ... Xil. 
 Broken River Aa aa of Clarke 
 River) .. ... 19, 28, 34, 36, 39, 43, 47, 48, 
 
 50, 51, 60, 61, 62, 63, 64, 120, 
 137, 178, 196, 521, 582, 610 
 
 Brovinia ... ae A Bie SoA 105 
 Bulgroo sie ifs ate ae 514, 556 
 Bullock Creek ah et He seat YE 
 Bulloo River aa Bee aaa 406, 513 
 Bundaberg ... ie os ao EXO 
 Bundanba ... 313, 316, 333, 335, 341, 
 
 343, 344, 349, 351, 352, 
 353, 366, 369, 370, 389 
 Bundilla ... eae at we «= 482 
 
750 INDEX TO PLACES. 
 
 Page. 
 Bungeeworgorai .., 391, 406, 410, 456, 457,458, 
 459, 460, 466, 479, 481, 512 
 
 Bungil Creek - fe (002 
 Bunya- Bunya Range By yabuks ill 
 Burdekin River _... Oe Xia ppodeooas, 
 
 39, 43, 47, 50, 58, 59, 65, 66, ; 
 
 120, 132, 133, 134, 516, 517, 
 521, 581, 583, 608, 722, 736 
 
 Burenda re : a 429 
 Burleigh Heads ae ine 350, 544 
 Burnett District ... re Ville, 1K.) Sey 40 8 
 Burnett River ae ad ... 811, 312, 314 
 Burra se &: i at ee 17, 
 Burranbilla... ae wes 428, 480 
 Burrendilla ... Be: A eae bal 
 Burrum LX Rees 95, 190, 300, 313, 
 
 ar 351, 352, 354, 356, 356, 
 359, 363, 367, 369, 370, 373, 
 396, 518, 620, 545, 740, 741 
 
 Bynoe River re see Dar 
 Byrinnia_ ... ee is ee . 404 
 CABBAGE-TREE CREEK ... ee ) 
 Caboolture ... aft on Arie yil., 34 
 Cairn Range ee AS aa son» eee) 
 Caiwaroo... ee ee falerl 
 Caledonian Creek, Etheridge .» 28, 522, 523 
 Caledonia Station, Aramac re a e426: 
 California Creek ... sa an Seo) Pe 
 Callide Creek A van : Fille Soy, 
 Calliope eA : Ke 85, 89, 107, 169 
 Cambooya ... aa ne oe a 
 Cambridge Downs ... a ae 413, 49 
 
 Camel Creek ae fe 2 40, = 
 Camisade Creek .. 542, 615, 622 
 Campaspe River... sr et Bape = Lay: 
 Campbell’s Creek ... we 604 668 
 Canal Creek ae: Re : nae | et a 
 Cania ae 3 X,, X11-100, 05, 
 
 107, 108, 109, 236, 240, 24.4, 
 252, 255, 264, 540, 543, 593 
 
 Cannibal Creek... a 24 
 Canoe Creek ne a = BAL 
 Canoona ... lis ae 137, 178, £96; 197 
 Canowindra, N.S. Wales ... me le 
 Cape Aberdeen ... se ia .. 548 
 Cape Bedford oe 529, 530 
 Cape Bowen wee is se ce Oe 
 Cape Cleveland... ee ate meee eke! 
 Cape Flattery = ae ae fe OEY) 
 Cape Hillsborough... nt we a) OA 
 Cape Melville ae Re a 530 
 
 Cape Palmerston 
 Cape River ... 
 
 , “B46, 614 
 
 ‘ “yiii., xii, 20, 23, 135, 
 “186, 516, 518, 519, 540, 582, 
 
 594, 706, 721, 730, 736, 737 
 
 : ; OLS, 617, 735 
 
 i 542, 614 
 ix., 527, 533, 540 
 
 Cape Upstart 
 Cape York ... ae 
 Cape York Peninsula 
 
 Capricorn Islands ... ee ae leiley 
 Carborough Creek ..., ah ie oen ee LOe 
 Carborough Range... . 168, 169, 528 
 Cargoon fx ae = ae 23, 582 
 Carl Creek , ae ice me we OO7 
 Carpentaria, Gulf of a ee 1, 606 
 Carron Range ae a ae we OAL 
 Cartwright Point aa 300, 305 
 Cave. Creek ... ae ae ae se) BP 
 Cawarra oF a ane hee BIO) 
 
 
 
 -Condamine River ... 
 
 
 
 : Page. 
 Cawarral ... _ Aa .. 91,110, 248 
 Cecil Plains.. ; POU 
 Cement Hill, Peak ‘Downes 32, Base 169, 193 
 Cerito Geen ee ss ae DLS 
 Charleston ... iS ae na 523 
 Charleville ... ' 416, 427, 512, 739 
 Charlotte Plains ... san IBN 
 
 1k. ei: 23, 25, 706, 708, 
 709, 725, 726, 730, 735, 736 
 
 Charters Towers 
 
 Cherwell Creek ... = a = 3805 
 Cheviot Range . i 513, 514 
 Chillagoe siG 119, 120, 121, 609, 789 
 Chinchilla 652, 653, 655, "656, 657, 
 
 658, 670, 67 79, 680, 682 
 Chollarton ... ve. pe 401, 445 
 Chowey Creek ae 3A 88, 101 
 Christmas Creek, Beaudésert ice S882 
 Clara Creek.. nee rh 514, 
 Clarence River, N. 8. Wales at ae A 
 
 Clarke Range 
 Clarke River i, Ee on 
 Claverton ... 7m oe . =~432 
 Clermont oe Xu 20, 31, 34, 42, 
 143, 158, 167, 169, 193 
 
 Clifton re sop otek, 341, 347, 350, 353, 386, 
 €05, 652, 666, 668, 677, 678 
 
 30, 144, 168 
 39 
 
 Cloncurry a» 20,11 2s9Gr aor 
 397, 401, 520, 712, 732 
 Coalbrook we. 897, 517, 582 
 
 Coen River, South .. one was 31, 541 
 
 Colinton vii., 313, 352, 353, 
 
 369, 370, 382 
 Collingwood er 500 aa ie Os 
 Comet River Ae a se) NGS 
 
 Vi. -vil., 34, 224, 341, 51], 
 590, "604, 631, 664, 665, 666, 
 667, 668, 673, 674, 675, 677 
 Conglomerate ss ss ee “ges: 
 
 Cooktown es ix., xt, b72, dae 
 “175, 178, 190, 193, 194, 365, 
 529, 530, 553, 555, 584, 591, 
 703, 704, 719, 730, 733, 735 
 Coolgarra ws ni xii., 705 
 Coomera River te 329, 544, 
 Coonabilla Creek ... oe Aer Rep aes 
 Coongalla ... a ar vor . 482 
 Cooper’s Creek... re “407, 517 
 Coorajah Creek... Ba aa w= «BA 
 Coorni Paroo River “ah it 7 oe 
 Copperfield River ... BoB: 
 Coreena ae : 405, 411, 422, 462, 482 - 
 Corinda > we om) AZ 
 Costello’s Creek des Sj pee NRL 
 
 Cracow Creek 143, “157, 158; Lea, 
 
 190, 191, 262, 286 
 
 Crawford’s Creek ... Aer ee OZ 
 Cressbrook ... sie a5 Ae Rrra aos: 
 Crinum Creek ie oar aa: OO 
 Crocodile... an 110 
 Crow’s Nest, near Mount “Morgan 90, 92 
 Croydon... : ... Xil, 14, 454, 
 
 "B25, 526, 540, 554, 555, 558, 
 561, 562, 563, 3 873, 702, 726 
 
 Culgoa River oe Sabie, AU | 
 Cumberland ee ane nee 15 
 Cumberland Tslands = nts sap a (enkG: 
 Cunnamulla au ee 416, 429 
 Cunningham’s Gap Pa 350 on wlan 
 
 Cunningham’s Range Se iat .. +629 
 
Cunungra Creek . 
 Curambin Creek 
 Curra 
 
 D’ AGUILAR RANGE... 
 
 Dagworth 
 Dalby cae 
 Dalgonally ... 
 Dalma * 
 Dalrymple ... 
 Darby Point 
 Dargalong ... 
 Darling Downs 
 
 Darlington Range ... 
 
 Darr River ... 
 Dart River ... 
 Dawson River 
 
 Degilbo Creek 
 
 Delaney River, Rikendse 
 
 Delaney’s C este 
 
 De Little Range oO Fletcher’s Creek 
 Diamentina River ... _ 401, 402, 514 Flinders Peak 
 Dideot Creek 88 Flinders River 
 Dinmore : Sea ms 342 
 
 Dingo Creek, Kangaroo Hise s vt 9 
 
 Dillalah sit Far As 431 Fort Bowen... 
 Dismal Creek 515 Fort Cooper... 
 Donor’s Hill ee 48) Fossil Brook 
 Don River, Bowen. 31, 215 Fraser Island 
 
 Don River, R ockhampton ... 
 
 Dotswood 
 
 Double Barrel Creek: 
 
 Doughboy Creek 
 Douglas Creek 
 Dray ton ‘ 
 Drummond Range... 
 
 Dry River, near Herberton 
 
 Dugald River 
 Dulacca Fae 
 Dulbydilla ... 
 Durham, Etheridge 
 Durilla Creek 
 Durundur 
 
 HAStERN CREEK 
 Eastwood 
 Edington 
 
 Eel Creek 
 Hidsvold 
 
 . Eight-mile Plains ... 
 
 Einasleigh River 
 Elbow Creek 
 Elgin Downs 
 Elizabeth Creek 
 Ellangowan. 
 Emu Creal... oe 
 Encrinite 
 Morgan 
 
 Endeavour River ... 
 
 England. 
 Escape Inlet 
 Esk River ... 
 
 wae Vi, ix. 4, 32, 34, 313, 352, 
 
 Creek, é 
 
 INDEX TO PLACES. 
 
 Page. 
 es as aor 329 Etheridge 
 ve , B44, Eton Vale .., 
 301, 305 
 Eukalunda ... 
 vii. Eungella ,.. 
 401 Evora Rot 
 Vii., ix., 605 
 625 Exmoor 
 89, 90 
 
 ., 517, 582, 594 Farr Care... 
 6 426 Fanning River 
 120 
 Farm Creek... 
 
 vee tee 
 
 751 
 
 Page. 
 
 xli., 15, 28, 29, 524, 702, 736 
 605, 664, 665, 666, 
 667, 668, 672, 677 
 See te a9 157 
 | 411, 424, 474, 
 
 483, 487, 515 
 
 168, 169 
 
 ees se 
 
 84; 35, 39, 43, 47, 49, 52, 
 65, 6 66, 67, 68, 69, 132, 616 
 : .. 840 
 
 379, 381, 604, 606, 633, 639, Fassifern 5 352, 370 
 
 642, 647, 654, 655, 657, 662, Feather-bed Range ak ate eS 
 663, 668, 670, 671, 673, 674 Fenestella Hill, near Mount 
 
 675, 676, 677, 678, 681, 683 Morgan 90, 92, 98, 210, 218, 219, 252 
 
 es ec ee BBY Fern Island... % 542 
 
 : | 252, 424, 740 Finlayson Hills ae : 547 
 
 : 30 Finnegan’s, Etheridge... oa Zé 15 
 
 95, 143, 157, 158, 167, Fisher's Creek wee "399, 401 
 
 169, 178, 190, 191, 511, 590 Fitzroy Island 613, 615 
 
 LOS Fitzroy River : vii., 90 
 
 28, 522 Flagstone Creek, Beaudesert 5 GHD 
 
 vii. Flagstone Creek, Toowoomba 328 , 341 
 
 92, 93, 178, 
 228, 255, 284, 289 
 
 132 
 ts 4] Gatr’s LooKout 
 39, 521 Gayndah 
 40,521 Gebangle 
 664, 665 Geikie Range 
 
 32, 97, 138, 140, 178, 188, 
 189, 192, 196, 197, 198, 516 
 
 
 
 Germany 
 
 Friendly Springs 
 
 Georgina River 
 
 : 582, 594 
 
 5, 345, 516, 517 
 
 ., 393, 394, 396, 397, 399, 
 
 400, "401, 407, 412, 413, 475, 
 483, 506, 517, 518, 519, 581 
 oa wa 625 
 ne 168 
 
 aa ae 593 
 
 618, 621 
 
 515 
 
 892 
 95, 100, 106 
 87, 105 
 
 tA 541 
 418, 419 
 630 
 
 vey (8, JUS Gilbert River .. Vili. > xii, 15, 23, 28, 36, 137, 
 22, 391, 520 520, 522, 523, 524, 526, 540 
 te = «. 49 Giiliat River : joe, YA) 
 A406, 511, 512, 514, 515 Gladstone af vii., 714 
 = 3 15 Glanmire 411, 469, Ey 483, 494 
 513 Glasshouse Mountains 5, 73, 739 
 Vii. Glastonbury TAA eee 
 Glendower ... , 407, 412, 506 
 .. = 401 Glenelg ye See re at te xi. 
 336, 341 Glen Linedale ae a poe A 6 
 431 Gloucester Island ... 613 
 544 Gogango Creek... ape er soe. BOY 
 xi., 16, 88 Goldsmith’ 8, Etheridge ... vee 15, 522, 523 
 Me 647, 740 Goodna , 334, 335, 341, 342 
 30, "38, 582, 583, 5938, 626 Gooroomjam oils, LSS PLT 
 - 34, 73 Gordon Downs Hiss: 396, 410, 478, 480, 485 
 140 Gowrie Creek ...604, 649, 651, 652, 653, 656, 
 391 664, 666, 667, 668, 669, 672, 
 404, 514: goes 674, 677, ite 680, 681 
 , ae 518, 605 Gracemere ... 90, 91 
 near Mount Grandchester oss ao 348, 544 
 ... 90, 92, 93, 210, 252 Grant River : ae ie 30 
 .. 529, 580, 588, 591 Gray Creek ... 38 
 142, 396, 409, 418 Greendale ee see, US, 
 or aie ae 541, 542 Greenvale ... ioe 40, 521 
 Pe 7, ... 851, 365, 370 Gregory Downs ,,.., ey, ay om Loot 
 
752 INDEX TO PLACES. 
 
 Page. 
 Gregory Range «. : 28, 525 
 Gregory River, near Maryborough Pe 2 DUD 
 Gregory River ule te ac 394, 475 
 
 Grey Range 390, 409, 454, 471, 
 
 488, 514, 550, 551 
 
 Grey’s Creek es 3 ; boxe oi Oek 
 Gumbardo ... a me a eee 
 Gunalda_... is es ; oe 30d) 
 Gunnawarra - 583, 584, 592 
 Gunpowder Cracks sae 397, 413 
 Guppy’s Tableland _ Be we oS 
 Gympie Vii., Xu., 34, 
 
 “70, 72, 87, 160, 177, 178, 
 207, 218, 219, 222, 224, 229, 
 230, 231, 233, 234, 239, 246, 
 248, 267, 268, 272, 276, 277, 
 278, 279, 281, 282, 287, 291, 
 292, 544, 595, 596, 728, 736 
 
 Hart Creek ea oe Sie Jou WG? 
 Halifax Bay Hn ase ae a 9 
 Hamburgh Creek ... are ise Nae pole 
 
 138, 624: 
 135, 136, 137, 196 
 
 Hannam’s Gap... 
 Harvest Home acc 
 
 Henderson Creek ... Aare a 542 
 Hendon re ats +7 Peron) 
 Herbert River 522, 588, 586, 613 
 Herberton ... x., 5, 584, 
 
 592, 720, 727, 735 
 Highfields ... a ee hh 
 
 Hinchinbrook Island be OLS 
 Hodgkinson... : Xs nee 121, 178, 
 
 196, 201, 527, 540 
 ... 8389, 841, 511, 604, 668, 672 
 ive | 405, 424, 515 
 
 Hodgson’s Creek 
 Home Creek 
 
 Hood’s Range sae He stele .. 514 
 Hookey Creek ace xe a8 oo oOD 
 Hughenden.., 394, 396, 397, 399, 401, 
 
 407, 409, 412, 462, 489, 
 494, 495, 505, 517, 555 
 
 Hungerford... ae ane 75 .. 514 
 Hunter Island sir nti ao we. 84, 42 
 Hunter River, N. 8. “Wales iis a aT 
 ILFRACOMBE a is = 503 
 India we ae be 409, 417, 520, 653 
 Inniskillen ... or aan head 
 Innot Creek... bite 0 is bf O29 
 Ipswich... 468 : vii., 5, 300, 311, 
 
 312, 316, 317, 321, 333, 346, 
 352, 3938, 354, 355, 356, 357, 
 359, 364, 387, 388, 390, 396, 
 414, 434, 441, 520, 54d, 597 
 
 Irvinebank ... - ae 6, 118 
 Tsaac’s Creek ae = 668 
 Isaacs River Anae SUPR 143, 167, 168, 169, 528 
 Isis River foe BOOST “45, 545, 
 
 554, 563, 564, 566 
 JANE’S TABLELAND a a a) (Doo 
 Janet Range alee vee ee man OAM: 
 Jardine River me ay a Canoe: 
 Jeannie River a: Ror a woe tu) 
 Jericho nae . at ah de 515 
 Jibbinbar ... ise ee ooo ae xi. 
 Jimbooinba .., an ee 329 
 Jimbour oat _ 347, 350, 604; 
 Jimna Se Rare vii., 18 
 
 Jirking Creek ee 404, 411, 462, 516 
 
 
 
 
 
 
 
 Page. 
 
 Johannsen’s Caves, Rockhampton xiii., 91, 
 611, 635, 645 
 Johnstone River 586, 590, 598 
 
 Julia Creek ... 397, 400, 413, 486, 625 
 
 KABRA bre re rei ia 91 
 Kamilaroi | 397, 413, 504 
 Kangaroo Hills xiii, 7, 39, 134, 521, 522 
 Kannagan Range ... 1. me OR 
 
 88, 178, 234, 243, 244, 245 
 39, 129, 182, 133, 
 ane 178, 244, 268, 264 
 
 Kariboe Creek 
 Keelbottom River ... 
 
 Kendal River a ; .. 940 
 Kennedy River... at ae 531, 538 
 Keppel Island, North wa ac aoe OL 
 Kerguelen Land... ee Se oe 
 Kileoy BSA a7 sft 351, 352, 369, 370 
 
 Kilkivan : Ke Key So. 87, 97, 98 
 
 King’s Creek 595, 642, 647, 
 "648, 651, 653, 661, 662, 663, 
 * 664, 668, 636, 667, 672, 678, 
 
 674, 675, 676, 678, 680, 682 
 
 Kingston... a“ : 325, 327 
 Kinrara Creek ah aes oa oe OSG 
 Knapp’s Peak .... Sat Ss ri 5 
 Kooingal 35, 89, 178, 202, 206, 268 
 Koorboora ... al a xii., 6, 119 
 Kroombit 88, 107, 109, 234, 
 
 243, 24:4, O45, 273, 593 
 Kyabra oes “8 514, 556 
 Kynoona ... Bee 6 ase ie | SOL 
 Lacaian River, N. 8. Wales... ve =A 
 Laidley 7 ; ' w= 4, 823, 544 
 Lake Tae aoe we ae i 43686 
 Lake Lucy . ae sists 41, 134, 522 
 Luke Mueller’ me us oe MED TS: 
 
 Lake’s Creek, Rockhampton .. 90, 91,92, 
 178, 218, 295, 296 
 Lancewood Range ... 30 ve Sol 
 Landsborough River 411, 462, 463, 464, 
 
 498, 501, 502, 503, 517 
 
 Lane’s Creek as in B24 
 Langlo River ne i DOO: 
 Langmorn 35, 89, 90, 178, 201, 610 
 Lansdowne ... . 425 
 Last Call, Cloncurry Ae Fr 21, 149 
 Laura River : . 529, 533, 536 
 Lee Creek ... he nots ee 38 
 Leichhardt Distr ict rs ae Rete! bay 
 Leichhardt Downs... . EO 
 Leichhardt River 1168, 397, 413, 462, 504 
 Leuten Downs 167, 169 
 Leyburn ... an sie OO 
 Lilymere ... ae 89, 90, 92, 225, oe 287 
 Limestone Creek, Mitchell Riv er. Pe bi hy da 
 120, 527 
 
 Lion Creek . Pe baie ie oe 90 
 Littabella Creek "300, 546 
 Little Kennedy River, Cooktown... 2a O28 
 Little River, Gooktown woe Sy 172) 176 
 176, 178, 194 
 
 Liverpool Plains ... as ae ia 695 
 Lizard Island vhs oe Ke ce [OLS 
 Lochaber ... aes 500 Nia a 88 
 Logan Downs : 157, 158 
 Logan River 4, 324, 350, 543, 544 
 Lolworth ee 28, 582, 594 
 
 Lord’s Tableland i” 606, 661 
 
Lornesleigh ... 
 Lowood ae 
 Lucky Valley 
 Lukin River 
 
 Lynd River... 
 Lynd Station 
 
 MoCoy’s Creek 
 Macintyre River 
 Mackay 
 
 "148, 146, 157, 167, ‘iss, "169, 
 
 INDEX TO PLACES. 
 
 Page. 
 
 eee . 135, 186, 296 
 
 vee eee . = B46 
 
 ; viii. 34, 73, 74, 112 
 ues Se 533, 540 
 oe wee 521, 593 
 res # 38 
 
 a 523 
 gers 390 
 O07, 
 
 546, 622, 710, 711, 713, 716, 
 
 722, 7 725, 728, 732, 734, 735 
 
 Mackenzie River ... ‘ 143, 169 
 McKinlay , .20 
 Macpherson Range... 4, 350 
 Mackinlay River ae 421 
 Magnetic Island Salhi 173, 613, 616, 710 
 Magowra te % OL 7 
 Malbon-Thompson Range. pa aa ioe 
 Malta a oat ah : 406 
 Malvern Hills Pe 4ok 
 Manfred Downs 407, 413, 416, 
 417, 420, 506, 625 
 
 Manning River, N. 8. Wales uae 46, HEY 
 Manoa Creek : Be 516 
 Manuka 422 
 
 Maranoa River 
 
 Marathon 
 
 Marble Island . 84, 42 
 Marburg 346 
 Marengo a Pity ou 
 Marlborough re fa aed a 34. 
 Maroochy River... see on swe 4 
 Maryborough ‘ .. 800, 396, 409. 
 
 454, 457, 458, 479, 544, 
 
 554, 555, 560, 562, 574 
 Mary River ... 4, 305, 544; 
 Maryvale 582, 606, 608, 632, 641, 
 
 642, 644, 652, 668, 673 
 Maxford ge) awee 
 Maxwelton ... _ 412, 419, 503 
 Mayne River 514, 556 
 Mazzlin Creek ees wa 3 586 
 Meerschaum Mountain ... sai s. | 330 
 Melville Plains sae #3, stor Aakete} 
 Mihi Sa ie meas 336, 343 
 Millie 5 “er ao feo, a0!8) 
 Milo : 513, 602 
 Minmi 404, 410, 454, 475, 481 
 Mitchell (S. ‘and W. Rly.) as 410, 429, 
 
 Mitchell Downs 
 Mitchell River 
 
 404, 409, 410, 475, 
 479, 480, 488, 501, 512 
 
 ...394, 396, 399, 400, 401, 407, 
 
 409, 412, 421, 441, 462, 463, 
 464, 466, 496, 508, 509, 555 
 
 4.46, 451, 472, 479, 
 
 482, 486, 501, 511 
 
 .. 440 
 
 at 1y, 120, 123, 176, 393, 512, 
 
 520, 527, B54, 559, 631, 712 
 
 Miva Creek ... 305, 341 
 Moggill xil., 333, 341 
 Molangul 18 
 Moondilla xii., ., 407, 427, 602 
 Moreton Bay Ae! 618, 621 
 Moreton District ix., 4, 34, 74, 
 Morgan River fe ye Gye 
 Morgan Tableland .., 530, 592 
 Morinish <n aa is Soe a) 
 Morven fs 5 512, 514 
 
 22 
 
 Mount Abundance... 
 Mount Adolphus Island 
 
 Mount Albion 
 Mount Barney 
 Mount Barren 
 
 Mount Bartle Frere 
 
 Mount Beckford 
 
 Mount Biggenden ..,. 
 
 Mount Black 
 Mount Bopple 
 
 Mount Bridgman ... 
 
 Mount Britton 
 
 Mount Browne 
 Mount Clara 
 Mount Conway 
 Mount Coora 
 Mount Corby 
 Mount Cordeaux 
 Mount Cornish 
 Mount Cotton 
 Mount Daintree 
 Mount Divlin 
 Mount Edwards 
 Mount Elliott 
 Mount Esk ... 
 Mount Fox ... 
 Mount French 
 Mount Funnel 
 Mount Goolman 
 Mount Hogan 
 Mount Holly 
 Mount Illalong 
 Mount Jukes 
 Mount Lang 
 
 
 
 Mount Larcombe * 
 
 Mount Leslie 
 
 Mount Leviathan .., 
 
 Mount Leyshon 
 
 - Mount Lindsay 
 
 Mount Lyon 
 
 Mount McConnell ag 
 
 Mount Macedon 
 
 Mount Mandarana.. j 
 
 Mount Mitchell 
 Mount Morgan 
 Mount Mulligan 
 Mount Nation 
 Mount Nicholson 
 Mount Ossa 
 Mount Perry 
 Mount Pleasant 
 
 Mount Razorback ... 
 
 Mount Shamrock 
 Mount Spencer 
 Mount Spurgeon 
 Mount Stanley 
 
 Mount Stewart, Grey Ranges 
 Mount T exibporine 
 
 Mount Toussaint 
 Mount Victoria 
 Mount Wheeler 
 Mount Wyatt 
 
 Muckadilla ... 
 
 Mudgeeraba Creek ‘ 
 
 Muldiva 
 Mulgrave River 
 
 753 
 
 we. = 414, 511, 512, "355 
 . 542 
 
 'B, 118, 121, 739 
 Re 5 
 560 A 547 
 
 ae Re 122 
 
 : " 899, 517, 582 
 xii., 87, 102 
 
 519, 582 
 
 305, 306 
 
 are 147, 169 
 
 157, 178, 208, 232, 233, 
 234, 235, 239, 248, 252, 254, 
 poses 264, 270, 273, 293, 548 
 ei OLD 
 
 98 
 
 .. 028 
 
 i 97, 98, 99 
 410, 454, 459, 555 
 
 4 
 
 “5 _ 411, 464, 502 
 
 2 328 
 
 539 
 
 144. 
 
 5 
 
 710 
 
 Sno OF GHB: 
 
 134, 585 
 
 oe 5 
 
 548 
 
 50 ». 15, 29,523 
 =e ae oe 88 
 169 
 
 547 
 
 Ne ee : 585 
 ue ocr ree 107 
 168, 528 
 
 “si 22 
 
 ee a 
 
 ae eh 
 
 _ 138, 136, 196 
 144, 145 
 
 546 
 
 oe 4s, Bb 
 Xiil., 542, 598 
 "176, 527 
 
 : 5228 
 520 
 
 548 
 
 Palys sete 
 
 he B42 
 584, 586 
 
 X., xli., 88, 106 
 ; © 169 
 638 
 
 ‘ 332 
 
 471, 488, 551 
 328, 329, 330, 350, 544 
 aes ’ 144, 145 
 _ 216, 269, 542 
 
 Ab viii., 110 
 
 Vill., ol, 95, 136, 
 
 137, 178, 196, 197 
 
 416, 428 
 
 544 
 
 xr 119 
 
 122, 592 
 
 BS Cope. ds 
 
754 INDEX TO PLACES. 
 
 Page. 
 Mullet Creek eee 554, 562 
 Munegai sg a oo Ba sae 17 
 Mungallalla ‘Ke ae ie rat enell 
 Mungar ee Fac oe Art Fe SUD 
 Munna Creek 87, 805 
 
 Murphy’s Creek ie 321, 338, 362 
 
 Murweh Ee ees nee re 428 
 Muttaburra ... ee 411, 425, “465, 478 
 Myall Creek at sak .. 605 
 NANANGO ... 
 
 Nebo Aoi 143, rye 167, 168, 178, 190 
 Neelia Creek M5 . 400, 411, 462 
 Neerdie a. ane Sc Aor, “ealll, 85, 305 
 Nerang Creek 3 ie 543, 544: 
 Neurum-Neurum Creek ... Se awaits 
 
 Newcastle Range ... 28, 522, 523, 524, 593, 629 
 New Guinea Xil., xlii., xiv., 614, 643, 
 684, 690, 712, 714, 719, 
 
 721, 732, 734, 735, 736 
 
 New South Wales ... 20, 34, 39, 45, 58, 
 58, 60, 61, 70, 74, 97, 141, 
 
 142, 168, 170, 171, 176, 200, 
 
 ee 247, 254, 259, 262, 2638, 
 
 278, 279, 281, 296, 314, 315, 
 
 341, 349, 357, 359, 360, 362, 
 
 365, 368, 371, 872, 382, 388, 
 
 390, 407, 417; 431, 528, 554, 
 
 596, 614, 617, 618, 637, 
 
 643, 723, 724, 728, 733, 734 
 
 New Zealand 317, 361, 608, 628 
 
 Nicholson River... ee Sey YI 
 Nickavilla Si 514, 556 
 Nigger Creek, Herberton Woe son 0,92 
 Nive River ep br 408, 411, 481, 515 
 Nogoa River ae ee bon 
 Noorama sis sae af 428, 430 
 Noosa , ; Ss A aA saith, 
 Normanby, Bowen.. Ao sa bee Xs, OO) 
 Normanby, Bur nett Bi ss ie 18 
 Normanby, Palmer 6 “123, 520 
 Normanby Range, Cooktown... a ee! 
 Normanby River see ... 529, 530, 533 
 
 Norman River 520, 524, 
 
 
 
 Normanton . j Ae xil., 526 
 Northampton Downs ... 405, 426, 462 
 Northcote ... ry) aie Ae bs 121 
 Northumberland Islands ... 5 84, 4:2 
 Norton Ao Kes , 107, 108, 109 
 Nudgee 617, 618, 635, 640, 641, 643 
 OAKEY CrEEK, BURDEKIN ae : 521 
 
 Oakey Creek, Cooktown 71, 172, 174, 175 
 176, 178, 190, 194, 520, 629 
 
 Oakey Creek, ree Downs ... we 604, 
 Oakhill ee me Sees 
 Oak Hills ... ; ot 5 40 
 
 Olsen’s Caves, Rockhampton XML, OL GLO; 
 
 635, 616, 646 
 
 Ooramera Creek ... ne re 305 
 Opal Range age iesie tes ests Bones ae! 
 O’Shanassy River ... St Ae a SYS 
 Oxley, near Brisbane F 596 
 Oxley Creek, near Hughenden 61g; 582, 738 
 Pappy’s GuuLy ... oe 38 
 
 Palmer xi, xIVv., 417, 128, 390, 
 409, 413, 467, 489, 
 
 493, 501, 538, 539 
 
 
 
 
 
 
 
 Page. 
 
 Palm Islands i ~~ 618, 719 
 Pandanus Creek ... re vee Bic 38 
 Paradise... Hc wae owe xu., 106 
 Paroo Range toe eee a0 Tee OLS 
 Paroo River is ah seh soe 40% 
 Pascoe River é tie : 541, 638 
 Peach River sae, OG 
 Peak Downs Gold and Copper Field 31, 33, 
 606, 635, 661 
 
 Peak Mountain, near Fassifern 3138, 352, 
 370, 373 
 
 Peel Island ... oo OLE, 
 Pelican Creek 144, 145, 150, 158, 169, 204 
 Pentland ... mee 3 ee 314 
 Pentland Hills a, sai ses EO MOd 
 Pera Head . 560 mate aaa "533 
 Percy Douglas Creek = ee soot Bie) 
 Percy Islands Sc ae ae 6138 
 Percy River... ae 38 522, 523 
 Piebald Mountain ... a si ie = aR 
 Pikedale ... 566 : % vi., 112 
 Pilton 55 te .. 605, 652, 663 
 Pine Creek ... . 380, 341, vil. 
 Pine Hill ie 138, 516 
 Pine Mountain . 345, 351, 369 
 Pioneer River 148, 546 
 
 Pitchery Creek , A axe 411, 509 
 Pitt’s Creek... a Bits “0 Harn E05: 
 
 Pleasant Creek ; bots Ns 513, 556 
 Point Danger : see act w= O44 
 
 Polygammon Creek pee ses .. Ald 
 Porcupine Creek Es . 399, 517, 582 
 Port Curtis District : : 35,610 
 Pring Creek Re Fr ane ee ALS 
 
 x., 35, 50, 88, 89, 
 
 RAGuan ace ae 
 90, 107, 109, 178, 610 
 
 Raine Island 2 . 614, 617 
 Rankin’s Creek ee ie ane oc 49 
 Rankin’s Mistake Creek ... Fe 2 OLS 
 Rattlesnake Island Ane as See LG 
 Ravenswood Ba _ ate Te 
 Reap Hook Range .. ¢ va BRT 
 
 Redbank, near Brianne 313, 334, 351, 352, 353, 
 367, 369, 370, 374, 381 
 
 ay abe 168, 528 
 
 : Pe . 584, 586, 592 
 19, 34, 41, 43, “At, 48, 50, 52, 
 54, at 56, 58, 59, 60, G4, 69 
 Reid’s Creek a6 : a 18 
 Return Creek aS a we 5 
 Richmond Downs ... 400, 401, 407, 413, 420, 
 463, 464, 483, 491, 503, 506 
 
 Richmond River, N. 8. Wales Rue é 4 
 Ridgelands, near Eeieenpees ves oe LA”) 
 Robertson River .» 28, 522, 523 
 Rockhampton Viii., xvi., 35, 70, 74, 89, 
 90, 92, 93, 110, 116, 178, 
 
 189, 196, 199, 200, 201, 
 
 : 208, 210, 211, 213, 216, 
 
 223, 226, 227, 228 230, 
 
 233, 235, 236, 239, 245, 
 
 246, 248, 256, 262, 263, 
 
 269, 271, 2745 286, 287, 
 
 288, 289, 290, 291, 292, 
 
 293, 294, 295, 296, 299 
 
 a 397, 418 
 ‘401, 404, 411, 447, 449, 462 
 
 Redcliffe Range 
 Reedy Brook 
 Reid River ... 
 
 Rocklands ... 
 Rockwood ... 
 
INDEX TO PLACES. 755 
 
 Page. 
 Rodd Bay ... bas wes ae cy G00 
 Roma ee ase w 1x., 404, 512 
 Roper Creek ae nee 157, 158 
 Rosenthal Creek .,. “ne Ai ste 74, 
 Rosetta Creek Ae af ; eLOLD. 
 Rosewoed, near Ipswich ... “311, 3138, 315, 
 
 337, 338, 343, 346, 350, 
 
 351, 352, 3538, 367, 369, 
 
 370, 371, 373, 375; 386 
 
 Rosewood, near Rockhampton — ...110, 318, 351, 
 "355, 856, 365, 
 
 366, 382, 384 
 
 Rossend 
 
 # Pe, 343, 344 
 Running Creek, Star, Burdekin ... 7, 129, 312 
 Running River... 7, 312 
 
 Russell River ., 122, 589, 597, 720 736 
 
 Saint Grorar River, MircHern 
 
 RIvER ... ba Sas nes See U7: 
 Saint Jean’s Station, Darling Downs 666, 668 
 Saint Lawrence nr S; te 95 
 Saint Paul’s Creek Ane a6 BP) 
 Saint Ruth ... .. 605, 668, 675 
 Saltern Creek ee 416, 423 
 
 ,sandgate ... re am “sa soo, En 
 Sandringham sh Ma Si 2 432 
 Seaforth ... OAS 
 Sellheim River  xii., 18, 138, 136, 528, 724, 734 
 Severn River ne. ix., 34 
 Sharrow... a Sic ons oe 683 
 Shelburne Bay ee re sre OY? 
 Sir William Thompson Range ie wwe «= OAL. 
 Skeleton Creek oe one a » 405 
 Soldier’s Cap aes ae a sa. BAD 
 South Australia... 20, 375, 
 
 390, 403, 404, 406, 407, 408, 
 409, 433, 450, 451, 454, 456, 
 457, 459, 474, 476, 479, 491, 
 549, 618, 623, 631, 643, 682 
 
 Spencer Creek se : vw. =14 
 Spicer’s Peak us a5 Sen 4 
 Spring Creek, near Toowoomba ... . ood 
 Springsure ., 143, 157, 158, 178, 260 
 Stanley River ne aoe vil. 
 Stanthorpe ... aie Sp as -, 685 
 Stanton Harcourt . ee LOU 
 Stanwell oe 91, 92, “167, SRE Ufo 
 
 190, 209, 210, 212, 215, 
 
 216, 218, 219, 224, 231, 
 
 234, 236, 243, 244, 245, 
 
 248, 252, 255, 256, 263, 
 
 285, 286, 290, 297, 355 
 
 Starcke River ’ 530, o 
 Starfield ee Ron wate no oye: 
 Star River ... ts Xe "39, 70, 96, 97, 
 129, 137, 177, 178, 196, 
 
 197, 208, 214, 215, 219, 
 
 234, 235, 236, 242, 245, 
 
 246, 262, 263, 264, 265, 
 
 275, 285, 291, 292, 709 
 
 Stewart’s Bore, near Tambo a! . 514 
 Stewart’s Creek, Stanwell... 171 311, 312, 313, 
 317, 343, 351, 352, 
 
 354, 355, 356, 364, 
 
 370, 873, 374, 376, 
 
 384, 518, 740, 741 
 
 Stewart’s Creek, Townsville .. 172, 178, 194 
 Stokes Range ah as “oF Old 
 Strathfield ... be =e om ne A2l 
 
 
 
 Page. 
 
 Styx River ... tee xiii., 95, 300, 308, 356, 
 309, "378, 376, 740, 741 
 
 Surprise Creek te wa 583, 593 
 Suttor River ., 185, 186, 168, 740 
 Sydney . 553, 614, 618 
 TALGAI : Vi., Viil., xi., 112, 318, 
 323, 352, 353, 373, 378, 381 
 
 Tallebudgera Creek A ww «BAL 
 Tamaree : Ce hor 83 
 Tambo 4085, 406, 411, 416, 424, 
 426, 471, 492, 514, 515, 516 
 
 Tanyalba Creek... na, GLUT 
 Tara .. 4 ca ee a oe 427 
 Taranganba.... se wee sal, BA! 
 
 200, 247, 255, 261, 
 ~ 268, 316, 317, 359, 360, 378, 
 383, 623, 643, 713, 729, 736 
 
 Tasmania eee 
 
 Tate River ... saa 413, 501 
 Teebar tee ane S06 * xil., 305 
 Telemon ... od nee eos 
 Temple Bay... se : , 542, 615, 622 
 Templeton River ... ae “00 Oa 
 Tenningering 5) U8 
 Tenthill Creek, near t Toowoomba... po, atte, 
 Terrible Creek Be Ss ; 35, 49 
 Thargomindah . 431, 631, 635 
 Theresa Creek ; 606, 661 
 Thompson River "393, 412, 514, 516, 518 
 Thozet’s Creek, see pags de 90, 91 
 Thurlagoona : acd ae 43 1 
 Thurles : nae a0 : 491, 512 
 Thursday Island ... sic ne w= B42 
 Tiaro ~ A $- fa SB ig 305 
 Tinaroo oes ee see ee sf 7 
 Tinnenburra Nee ie ve +» 430 
 Tivoli ee his 313, 336, 841, 344, 349, 
 
 351, 352, 353, 366, 368, 369, 
 374, ee 37 8, 383, 386, 396 
 
 Tomahawk Creek ... 40, 134 
 Toorak = aon Pal 
 Toowoomba vii., 313, 350, 352, 362, 379, 381 
 Tower Hill ... ; 411, 497 
 Townsville . 4, 172, 173, 7Sep lsd. 
 
 67, 618, 622 hee 639, 640 
 Traveston ... 5s. ane 
 T'revethan Creek, near + Cooktown-., aS 11 
 Tweed River, N. S. Wales x0 ae 4 
 Tynana Creek, Victoria... os fe 45 
 
 VALLEY oF Lagoons 40, 521, 583, 584, 585 
 Vegetable Creek, N. 8. Wales... 74 
 Victoria . 20, 32, 45, 60, 97, 142, 359, 
 "360, 372, 518, 575, 595, 597, 
 614, 618, 621, 643, 724, 740 
 
 Vindex 402, 421 
 
 WAIRUNA 
 
 oe 40, 41, 134, 522 
 Walker’s Creek 
 
 167, 168, 178, 
 190, 194, 319, 582 
 Walker’s Table Mountain... 412, 413, 463, 464, 
 491, 495, 496, 498, 506, 508, 509 
 
 313, 337, 341, 343, 345, 
 
 346, 349, 351, 364, 365, 366 
 
 re ag: ... 391, 392, 396, 
 
 399, 406, 407, 413, 446, 454, 
 
 456, 466, 478, 475, 476, 489, 
 
 493, 499, 501, 510, 520, 559 
 Walter’s Range... . «= B14 
 
 Walloon 
 Walsh River 
 
756 INDEX TO PLACES. 
 
 Page. 
 
 Walton 350 
 Wandovale ... 582 
 Warra Warra 667 
 Warrego Range : i 2 O13 
 Warrego River "404, 407, 411, 
 
 497, 511, 514, 516 
 Warrenda oe et ; ee ie) 
 Warriana ... 45 nae _ 412 , 462, 494 
 Warwick ; Bi 112,3 340, 345, 653, 656, 657 
 Waterford ... ; - 328, 544 
 Watertown ... Ses . 843, 344, 349 
 Watsonville... : ae sete Mea bgiar 8, 118 
 Watts’ Creek >» 402 
 Waverley 95 
 Wealwandangie ., 158 
 Weddin Mountains, N. 8. “Wales... 142 
 Weelamurra a : , ESI 
 Welcome Valley , 532, 533 
 Wellesley Islands ... 558 533 
 Wellington Caves, N. 8. Wales ... Uae O2e 
 Wellshot ... Pe ... 426, 497, 503 
 Werna ; 2 ost 402, 421. 
 Westbrook Creek ... 605, 648 
 Western Australia ... 390, 396, 434, 560, 643 
 Western Creek, Gilbert River ma” APS 
 Westlands ooh . 24 
 White Mountain Creek “519, 582 
 Whitsunday Island 613 
 Whitula e 432 
 Wide Bay Creek 99 
 Wide Bay District ix., 4 
 Widgee Creek 332 
 Wiembilla Creek 653 
 
 Wild River ... ade 
 Wilkinson Range ... 
 Williams River 
 
 ix., 6, 592 
 
 541 
 
 400, 401 
 
 
 
 
 
 Page. 
 Willie’s Range... Ace EK cece HOLE 
 Wilson’s Peak ae i aes se 5 
 Windeyer Creek ; 515, 541 
 W indorah ay as 513, 514 
 Winton ; 401, 402 AL, 421, 468, 514, 556 
 Withersfield F (om. VSSe740 
 Wokingham Creek... ma os 402, 514 
 Wolca * me realy) 
 Wolltunbilla SExIVe; 390, 393, 396, 399, ‘406, 
 
 408, 409, 414, 435, 436, 439, 
 
 440, 442, 443, 444, 445, 446, 
 
 44.7, 448, 449, 451, 454, 456, 
 
 4.57, 458, 460, 462, 466, 467, 
 
 os 469, 470, 471, 475, 476, 
 
 4.79, 480, 488, 484, 485, 4.86, 
 
 487, 488, 489, 501, 512, 555 
 
 Womallilla ... oe os Re ah 
 Wongalee 399, 401, 517, 582 
 Woolgar... ous . 15, 23, 28, 522, 524 
 Wrotham Park od 
 
 Wycarbah ai 313, 355, 356, 377, 382, 383, 386 
 SY LAACED Aue a “e6 ie 90 
 Yandilla . "604, 605 
 Yarra Basin, Victor ah : 20 
 Yarrabil Grsek fee (320 LOG 
 Yarrol > 36, ‘87, 178, 252, 255, 276 
 Yass, N.S. W Vales .. i. 20, 53 
 Yatlon ‘94, Tis 178, 229, 233, 
 241, 254, 257, 267, 278 
 Yeppoon... is ote 
 Yo Yo Creek ee wee ree 
 Yorke’s Peninsula, Ss. Acatralia a BEC 20 
 Yuleba ae ee aca wee Tee bile 
 ZILLMANTON 119, 120 
 
INDEX TO SUBJECTS. 
 
 
 
 
 
 SSS SS 
 Page. Page. 
 AGATE Bet fete es we ae 28, 145 Bowen River Formation, Middle, in the 
 Andesite... Ce eo ae a Assi ' ype District . 150 
 Antimony— Life of the Period ae 159 
 Eidsvold oo ne he so 16 Bowen River Formation, Middle, marth 
 Trvinebank AES Ramon Aan are 6 of the Type District alsy/ 
 Mitchell River aa a plate Bowen River Formation, HEPPe in the 
 Neerdie nes ay wi ace 85 Type District 16] 
 : 121 I 7 “6 L 
 Northcote aie aes 500 309 2 ata of the Pesiod 177 
 Pandanus Creek os ren a 38 : 
 pe 9 Bowen River Formation, Upper, outeide 
 Ravenswood ... Ms as Be 12 4 District 167 
 Arsenical Pyrites ... Loe ... 6, 11, 98, 101 ¢ Bee a ee istric oe ier 
 Artesian Water 321, 323, 414, 433, Blain At os 
 é eS air Athole 170 
 516, 526, 739, 740 Odskansuclt Benes 169 
 Ash and Agglomerate, Volcanic: ... 27, 105, Bee ae ie 2 
 9 Cement Hill, Clermont 169 
 144, 146, 148, 172, 173, few Riese 169° 
 321, 516, 533, 546, 548 “i SEN : 
 ; saacs River 169 
 New Guinea ... Ad Sa “5 LGhare! 
 Nati Lenten Downs.. 169 
 Tertiary aoe Fo ee eo ES Little Ri C ce pe 
 ES he Af 936 ittle River, Coo town 175 
 S: ae ee Mackay e ane 168 
 Mackenzie River 169 
 Basatt— fs : 
 Basalt Wall, Lolworth =... «.. 738 ne Greok, Cook i 
 Bowen River ... e x 144, 150 Bee ty Oo ul ak fi 
 AL Stanwell F er ital 
 Burdekin River hoe Re eee Le ‘ 
 CatclRiver 721 Townsville 172 
 Giitton be ib a ae ... 340 Burdekin (Middle Devonian Hormaton 34 
 Cooktown Re) wit ie ae List of Fossils from : : 43 
 Herberton wh 720, 721 Organic Remains of ... AT 
 Ipswich oe 333, 350 Burrum Formation oe she ... 3800 
 Mackay ... 146-149, 722, 725 List of Fossils.. 5 ia 811, 740 
 Mount Beckford as 3 abn = sly Description of the Species Ae 313, 740 
 Mount Black ... ce sto. IS) 
 New Guinea ... im ". 687, 719, 721 
 New South Wales... st ee oa es, CavEs me ne a4 Fe 91, 609 
 Oxley Creek ... ae an one. fists} Chaleedony .. 145 
 Palm Island ... Mee iF Jom. mOErAS) Classification ‘of Queensland Formations 3 
 Pleasant Creek ~ ae ngae © alls? Coal— 
 Rosewood, near Ipswich ee yess. Ayrshire Downs 402 
 Russell ey we 720, 736 Bee Creek 167 
 Surprise Chak x oor eer 20 Blair Athole =: 14 a 170 
 Tertiary an “e ae ae anDis Bowen River 151, 161, 163, 164, 166 
 Toowoomba ... ves 550 aay eae Brisbane : 321 
 Victoria ee an ve ee | REM Bundaberg 307 
 Bibliography ote ae 580 so nau eaten ala 406 
 Bismuth— Burrum ae 800 
 Cloncurry x a0 ace 55 21 Callide Creek . ie 357 
 Halifax Bay ... ane ae noe 9 Cherwell Creek | we OOS 
 Irvinebank ... Se en ise 6 Desert Sandstone, in ... ... 029, 582, 588 
 Kangaroo Hills ae see se 9 Dulbydilla 406 
 Mt. Biggenden a ae 87, 102 Flinders River 397 
 Mt. Shamrock ee me 88, 100 Gregory River ve OOo 
 Percy River ... ee en Bie 30 Ipswich Coal Field ... 822, 333, 347 
 Sellheim fete : sind 13 Isis River 305 
 Boioro Limestones, New Guinea .; OCG Jimbour 347 
 Bowen River Formation, Lower, in Lenten Downs 167 
 the Type District tad ae w. 144 Little River, Cooktown 175 
 Contemporaneous Volcanic Malta ... ; 406 
 Rocks A .. 144 Mitchell River! A ae O27, 
 Bowen River Formation, "Lower, Miva ... <r Pe 305 
 outside of the Type District... as 40 Oaky Creek, Cooktown me co. ave! 
 
758 INDEX TO SUBJECTS. 
 Page, 
 
 Coal—continued. Gold—continued. 
 Pelican Creek ... ree wae 150, 151 Cania ... 
 Rosewood Scrub Gc 346 Calliope 
 St. Lawrence .., soe 308 Cape 
 Stanwell iva Cawarral 
 Styx River = 308 Charters Towers 
 Tanyalba Creek 306 Clermont 
 Tiaro re 305 Cloneurry 
 Townsville 172 Coen 
 Vindex ‘ w» == 408 Crocodile 
 Walker's Creek 167, 168 Croydon 
 Werna. : oo 402° Desert Sandstone, under 
 Winton — 402 Hidsvold oe 
 
 Cobalt— Etheridge 
 Mount Coora ... Ec 99 Gayndah 
 
 Cone-in-Cone Structure , 393, 400, 4.01 Gebangle 
 
 Copper— Gilbert 
 Black Snake 98 Gooroomjam ... 
 Cloncurry 20 Gympie 
 Herberton 6 Hodgkinson 
 Mount Coora ... 98 Jimna ... 
 Mount Perry ... 17 Kilkivan 
 Peak Downs 33 Krombit 586 
 Pikedale 112 Lucky Valley ... 
 Strathmore 145 McKinlay 
 
 Coral Reefs, New Guinea .. re LOGS Marengo 
 
 Cretaceous .. 338 390, 686 Milton ... 
 Lower. See Rolling ‘Downs Molangul 
 
 Formation. Moondilla 
 Upper. See Desert Sandstone. Mt. Biggenden 
 Mt. Britton 
 DEPRESSION OF LAND 613 Mt. Leyshon ... 
 
 Desert Sandstone 
 
 Age of, and Life of 554 Mt. Victoria 
 Coal and Opals in 555 Morinish 
 Organic Remains of ... 557 Mulgrave 
 Devonian Formation, Middle 34, New Guinea ... 
 List of Fossils from .., ee 43 New South Wales 
 Organic Remains of ... 47 Normanby, near Bowen me 
 Diamond— nhc od near Mt. geet sad 
 Agate Creek (*) 28 Northcote 
 Dingo : 623 Norton * 
 Diorite 147, 148, 149, ilsiy¢. 125, 726 Palmer.. 
 Dolerite— Paradise 
 Bowen River ... 500 . 161, 163-166 Peak Downs, Clermont 
 Cape River District ... 737 Pikedale 
 Mackay 725 Raglan ... 
 New South Wales wee! Ravenswood 
 Pelican Creek .. 154, 156 Ridgelands 
 Sellheim River 724 Rockhampton ... 
 Dotswood Beds 39, 132 Rosewood ee 
 Drummond Beds 138 Russell River ... 
 Talgai ... at 
 ELEVATION OF LAND 614 Tenningering ... 
 Emeralds 741 Warwick 
 Wolca ... 
 FLUORITE 6 Woolgar 
 Yatton ., 
 GARNETS... 28, 730, 738 Granite and Granitic Rocks 
 Geological Maps, purpose of 4, Granite— 
 Argentine 
 
 Geological Surveys of Queensland, His- 
 tory of ... : er 
 Glacial Action 
 
 ‘| 124, 168, 170, 
 174, 176, 511 
 
 vi. 
 77, 151, 609, 618 
 
 Mt. Morgan 
 Mt. Shamrock... 
 
 C antibal Cr eek 
 Clarke Range .. 
 
 Gold— Cooktown 
 Black Snake be 98 Etheridge 
 Boolboonda bre ile: Herberton 
 Brovinia one ane S08 105 Janet Range ae 
 Canal Creek ... ne nn ie Mackay bis oe 
 
 Page. 
 
 88 
 a Oy 
 23, 518 
 
 110 
 
 23 
 
 169 
 
 20 
 
 30 
 
 110 
 
 14, 525 
 
 ", 589, 540, 543 
 ‘ch eats 
 
 15 
 
 100 
 
 105 
 
 a 28 
 ‘18, 110 
 74, 84 
 “116, 121 
 hae 18 
 97 
 
 109 
 
 112 
 
 20 
 
 30 
 
 108 
 
 18 
 
 ae Og Z 
 87, 102 
 elie 
 27 
 EOS 
 88, 100 
 Pree ay: 9) 
 110 
 122 
 689 
 171 
 30 
 18 
 122 
 108 
 539 
 106 
 31 
 Face. abe 
 88, 107 
 
 : Ly 
 110 
 
 110 
 
 110 
 
 597 
 
 112 
 
 18 
 
 112 
 
 17 
 
 28 
 
 a 111 
 4, 702, 729 
 
 123, 
 
 124 
 144 
 703 
 me orks): 
 Sie Dp 
 pape may! 
 146 
 
INDEX TO SUBJECTS. 
 
 Page. 
 Granite—continued. 
 Mt. Biggenden 102 
 Mt. Bopple ‘ 305 
 Mt. Bridgman... 169 
 Mt. Dalrymple 169 
 Mt. Spencer .. 169 
 Pentland Hills 5, 739 
 Teebar .. = 0b 
 Graphite... 96, 306 
 Greenstone of Gympie 77 
 Guano, Bat... 618 
 Gympie For mation, in Ty pe District 72 
 Gympie Formation, outside Type Dis- 
 trict— 
 Cania ... 88 
 Calliope 89 
 Chillagoe 119 
 Dee River... 92 
 Don River, Rockhampton 92 
 Eidsvold ‘ 88 
 Gebangle ae 87 
 Hodgkinson 113 
 F.. Kooimgal 89 
 Langmorn 89 
 Mt. Albion 118 
 Mt. Biggenden 87 
 Mt. Shamrock... 2 
 Mt. Wyatt 95 
 Palmer LZ 
 Raglan.. 88 
 Rockhampton ... 90 
 St. Lawrence ... 95 
 Silverfield 118 
 Styx 95 
 Watsonville 118 
 Yarrol . 87 
 Yatton ... 195 
 Gypsum 392 
 os 
 HoRNBLENDE Ee 736 
 Hypersthene Rock.. 738 
 Icr Action. See Glacial Action. 
 Introductory Chapter 1 
 
 Ipswich Formation— 
 In Type District 
 
 . 321, 333, 346 
 
 At Stewart’s Creek, Rosewood, and 
 Wycarbah, near Rockhampton .. 30D 
 
 Age and Relations 
 List of Fossils.. 
 
 359 
 
 351, 356, 362 
 
 Organic Remains, and Description ‘of 
 
 the Species .. 
 
 364 
 
 Igneous Rocks associated with 350, 9 740, 741 
 
 Tron— 
 Cloneurry Ge 
 Kangaroo Hills. 
 Running River 
 
 Krvort Grits, New Guinea 
 
 LEAD— 
 Argentine 
 Black Snake 
 Dry River : 
 Gilbert River .. 
 Trvinebank 
 
 Kangaroo afk 
 
 22 
 8 
 9 
 
 684. 
 
 45 
 eae 298 
 118, 126 
 30 
 
 118 
 
 
 
 Lead—continued. 
 Mt. Albion ... 
 Mt. Shamrock 
 Ravenswood 
 Running River 
 Sellheim ; 
 Stanton Harcourt 
 Yarrol ... 
 
 Leucite 
 
 Lignite 
 
 Lithomarge ... 
 
 MAMMALIA, Exrincr 
 
 Man, Geological History of 
 
 Manganese— 
 Kilkivan 
 Mt. Biggenden 
 Mt. Shamrock 
 Peak Downs 
 Running River 
 Sellheim 
 Marble— 
 Calliope 
 Chillagoe 
 
 N Seeinberiand: letands 
 
 Palmer ... 
 Reid River 
 
 Maryborough Beds. See Desert 
 
 Sandstone 
 Mercury— 
 Kilkivan 
 New Guinea . 
 Wide Bay Creek 
 Metamorphic Rocks 
 Molybdenite 
 
 New Guinrna, GEOLOGY OF 
 Paleontology of 
 
 Petrographical Notes ... 
 
 Nickel 
 
 OBSIDIAN 
 
 Opal— 
 Bowen River ... 
 Bulgroo ‘ 
 Cheviot Range 
 Grey Range 
 Nickavilla 
 Pleasant Creek 
 Kyabra... : 
 South Australia, 
 ‘Winton 
 
 PERMO-CARBONIFEROUS SYSTEM... 
 
 Fossils of 
 
 Description of the Species 
 
 Petrographical Notes 
 Pitchstone ... 
 Plutonic Rocks 
 New Guinea 
 Porphyrites — 
 Bowen River ... 
 Croydon 
 Gympie 
 Herberton 
 Mackay : 
 New South Wales 
 Tasmania 
 
 4, 19, 687 
 
 759 
 Page. 
 118, 125 
 88 
 
 12 
 7 
 128 
 101 
 87 
 733 
 689 
 10 
 
 604 
 622 
 
 97 
 102 
 101 
 
 33 
 
 10 
 
 13 
 
 89 
 120 
 42 
 Ray, 
 41. 
 
 . 800, 544, 554 
 
 98 
 689 
 98 
 
 102 
 
 684 
 690 
 
 712, "714, 719, 721, 
 734, 735, 736 
 
 99 
 732 
 
 145, 165 
 514 
 514 
 514 
 514, 
 513 
 514 
 552 
 514 
 
 70 
 
 178 
 
 179 
 
 699 
 
 736 
 
 .. 4, 144 
 688 
 
 144 
 726 
 728 
 727 
 728 
 728 
 729 
 
760 INDEX TO SUBJECTS. 
 
 Page. 
 Porphyry and Porphyritic Rocks os 4 
 Porphyry— 
 Brisbane (?) 5 
 Darling Downs 4 
 Flinders Peak 5 
 Glasshouse Mountains (2) 5, 73 
 Herberton as Ses 5 
 Kilkivan x bats ay 97 
 Knapp’s Peak 5 
 Mackay = 147 
 Macpherson Range 4 
 Maroochy River 4 
 Mary River 4 
 Moreton District 4 
 Mt. Barney 5 
 Mt. Cordeaux ,., 4 
 Mt. Edwards ... 5 
 Mt. Esk 5 
 Mt. French 5 
 Mt. Goolman ... 5 
 Mt. Lindsay ... 5 
 Mt. Mitchell ... 4,5 
 Spicer’s Peak ... 4 
 Townsville... 4 
 Wilson’s Peak e. Sas 5 
 Port Moresby Beds, New Guinea Soo, Lehel3s 
 Post-Tertiary iat ae 604, 635 
 Life of the Period Shc a we | 682 
 Organic Remains of ... on 639, 740 
 New Guinea ate 685, 690 
 RarisED BEACHES .. 614, 684 
 Recent 604, 684 
 Rhyolite Pe ‘712, 730, 735 
 Rolling Downs Formation (Lower Creta- 
 ceous) ‘ ; abi a fon BAU) 
 List of Fossils see nas .. 409 
 Organic Remains of .., ae we = 484 
 Ruby (?)... oF Soc 53 Sr 28 
 Sanp Dunes 506 ane ane ; 621 
 Sapphire “28, 741 
 Serpentine ... 97, 98 
 Silver— 
 Argentine ASD AGS aa 36 45 
 Black Snake ... nod an Re 98 
 Croydon Ave +H zy Ae 14 
 Dry River : one ros 118, 126 
 Gilbert an ane Suc Shs 30 
 Irvinebank ... 88 Hos LS 
 Kangaroo Hills om ik ce 7 
 
 Mt. Albion Aa Ss 118, 125 
 Mt. Shamrock ... ae Abe asa 88 
 
 Ravenswood ... ee eee as 12 
 
 Running River As as ee vi 
 
 Sellheim Aa cae as “ 128 
 
 Stanton Harcourt “eA aes ae 101 
 
 Yarrol ... a re ts os 87 
 Springs— 
 
 Thermal ... 415, 624, 687 
 
 Mound Springs we 433, 624 
 
 At base of Desert Sandstone. 513-515, 525 
 Mount Morgan, an extinct Thermal 
 
 Spring ae abt avs vo. SIE) 
 
 Star Formation aw ae 39, 129 
 
 List of Fossils from ... net —» 41 
 
 Page. 
 
 Sulphur... vee a 
 Syenites and Syenitic Rocks 
 TACHYLITE . fr 732, 735 
 Tertiary— 
 South Australia : 550 
 Volcanic Rocks and Drifts referred to 
 Tertiary Period E: 575 
 Thermal Spring Deposit (Mt. Morgan) 
 referred to Tertiary Period a 
 Plant Beds near Oxle ze 596 
 
 New Guinea 
 
 685, 690, 697 
 
 Victoria 740 
 Tin— 
 Annan River ... 10 
 Bloomfield River 10 
 Cannibal Creek 124 
 Hidsvold 16 
 Hinasleigh River 30 
 Herberton 5 
 Trvinebank 118 
 Kangaroo Hills a 
 Mt. Spurgeon ... 638 
 Pascoe River ... 638 
 Running River : vi 
 Russell end J ohinstone Rivers 598 
 Stanthorpe 635 
 Watsonville 118 
 Tonalite BE 
 Topaz 5, 28 
 Tourmaline— 
 Annan River El 
 EHidsvold Ae 16 
 Cooktown 704, 735 
 Trachite— 
 Darling Downs 4, 
 Gladstone 714 
 Glasshouse Mounteines 739 
 
 Mackay District 
 
 "546, 715 
 
 New Guinea 687, 714 
 Trias-Jura System . ; . , 800 
 Lower (Burrum) Formation.. 300 
 
 Organic Remains of Burrum Forma- 
 
 tion, and Description of the Species 313 
 Upper (Ipswich) aes 
 in Type District . 821, 333, 346 
 List of Fossils . 851, 356, 362 
 Upper (Ipswich) Formation, ‘outside 
 of Type District ne 355 
 List of Fossils - 356 
 Upper Formation, Organic Remains, 
 and Descriptions of the Species ... 364 
 Vorcanic Activity In New GUINEA... 688 
 Wo.LFraM 6, 10 
 
 White Trap in Coal Seams 
 Wood, Fossil 
 
 ZINo— 
 Charters Towers 308 es aS 
 Dry River : soc sat . 
 Mt? eA bionmamaes ate ee sae 
 Mt. Perry 3 
 Ravenswood 
 Stanton Harcourt 
 
 Zircon uae 
 
 "185, 166, 161 
 165, 166, 168, 175 
 
 27 
 
 + 126 
 126 
 17 
 vail 
 101 
 741 
 
INDEX TO THE GENERA, 
 
 SPECIES, AND PRINCIPAL SYNONYMS 
 
 
 
 N.B.—A heavy figure denotes the page at which a Genus or Species is described. 
 
 The Synonyms are in italics’ 
 
 
 
 Page. 
 
 ACTHON ... a8 we 484 
 a depressus “410, 411, 484 
 <2 Hochstetteri ae 484, 
 Actinocrinus is ‘ mee 07, 
 5 sp. ind. 93, 129, 187, 
 141, 180, 207 
 Adrana F.) b66 
 » elongata 554, 566 
 Aeschna ae w= AAT 
 x flindersensis . 899, 412, 441 
 Alethopteris 3 ose hills 
 fe australis 311, 312, 316, 352, 
 354, 356, 359, 360, 362, 370 
 + Lindleyana ... 352,354, 362, 370 
 rr odontopteroides 368 
 Alveolites ... ei or. ne 52 
 s alveolaris a8 43, 48,53 
 
 . 7 var. queens- 
 landensis 43, 48, 54 
 f robustus... tes 43, 47, 54 
 s ep: ind... w. 43,47, 54 
 Alveopora, sp. ind.... ae eae gevee GOL 
 Ammonites ... a, nor ans 4.92, 697 
 » - Beudanti, var. Mitchelli 3895, 494, 
 AS Daintreei we ... 090, 412, 495 
 » Flindersi 394, 411, 412, 413, 494 
 Fe inflatus Per ..411, 412,493 
 os Sutherlandi ... 394, 412, 413, 496 
 3 walshensis .. 493 
 Amphipeplea vinosa 644, 
 Amplexopora se a “ 55 
 _ ? Koninckii... , 43, 48, 55 
 Amplexus ... see — mc % 60 
 a Sp.and..... 44, 48, 6O 
 Amusium ... We sor ee 447, 
 rs SP MIG we 112, 447 
 Anas re aii sor, we oles 
 » elapsa Ae noe 655 
 Anchura _... rer ae ed .. 486 
 »  ? Wilkinsoni a yas 411, 486 
 3 espana: a .. 486 
 Ancyloceras me Be nee AZ 
 s Flindersi 394, 406, 411, 
 
 412, 413, 497 
 
 g Soa! 413,498 
 Aneimites : LOL 
 _ austrina... 140, 141,191 
 Angiopteridium . 375 
 Ph ensis ee otis 
 
 sp. ind. 352, "854, 362, 375 
 Anomalocardia ‘ uve) G41 
 . trapezia ... 641 
 Areopora ... aes vs , 57 
 » australis des 43, 47,57 
 
 Page. 
 Araucarites .. wal soo ote 8 
 3 polycarpa | 856, 363, 383 
 Araucaroxylon : Pe as Pre oie Ls | 
 a _ Nicholi ae tes 
 Arca ass me .» 468 
 #5 lohata . 641 
 b plicata ee ats 449 
 » ? prelonga : 410, 468 
 ,» trapezia ae re es Ri Oak 
 Sate 695 
 Archeocidaris Son aks: 
 3 sp. ind. ‘93, 94, 180, 213 
 Archizonurus ie a se oval 
 ‘3 securus 5d ie aan Aaya 
 Arenicolites ... 297 
 Argiope a : eee 44.2 
 Rahs ae punctata .. . 409, 443 
 Mee Wi éllumbiliaensis 409, 442 
 Aspidorhynchus ... oe 0 412, 504 
 Astarte ot ee : s 471 
 »  wWollumbillaensis ... nas 410, 471 
 Astartella — ee 276 
 be ? rhomboidea 84, 184, 276 
 Astartila eT: 
 » cytherea "159, 184, 277 
 Asterocalamites Me LSS 
 i scrobiculatus 140, 141, 178, 189 
 Athyris xf es see w. 248 
 »  ambigua d5 88, 182, 243 
 
 "" 88, 182, 243 
 
 » Randsi 
 
 »  Roysii 92, 182, 243 
 Atrypa rs rs 65 
 »»  desquamata... 47,66 
 
 » ‘reticularis ... 44, 47, 65 
 Atys titel ms ee acer Oy 
 job ake 5a ae fee see 695 
 
 eer 460, 696 
 
 395, 397, 399, 
 
 ee ughendenensis o 
 400, 404, 405, 406, 409, 
 
 411, 412, 413, 460, 461 
 
 + tiga pany 409, 4.60 
 Aulopora, sp. ind. 64 
 Avicula equalis “449, 453 
 a braamburiensis ee 408 
 
 »  Barklyi 409, 452, 453, 455 
 
 : » var. reflecta 457 
 
 Ma corkion sisi "., 409, 458, 458 
 
 >» curta a ne ~ a eB 
 
 »  hughendenensis ; 395 
 »  orbicularis ae 409, 451 
 » reflecta . 409, 453, 457 
 5 simplex 449, 453 
 + substriata... 453, 459 
 
 "., 409, 453, 458 
 
 »  wmbonalis ... S56 
 
762 INDEX TO GENERA, ETC. 
 
 Page. 
 
 Aviculopecten ve 8 a0 eee Ae659) 
 PA illawarrensis ier Sou Aa, 
 
 es ? imbricatus . 84, 184, 26'7 
 
 ~ Laurenti 92, 93, 94, 184, 268 
 
 3 limeeformis... 84, 95, 159, 184, 266 
 
 _ multiradiatus. 84, 89,184,268 
 
 3 subquinquelineatus 159, 184, 266 
 BAIERA ee Bie are aPC OLS 
 bidens te 312, 318 
 Banksia wes ie ane as Ro isleys 
 Baylea Konincki ... ses AG “aot paetetsl 
 Belemnitella diptycha 394, 490 
 Belemnites ... . 487, 545, 574 
 = australis 409, 410, 411, 48'7 
 
 > Barklyi Soe .. 489 
 
 5 Canhami 394, 406, 409, 411, 
 
 412, 413, 490 
 
 = eremos... 409, 410, 488 
 
 ” Oxys 411, 488 
 
 5 paxillosus 408, 4:88 
 
 x Sellheimi .. 897, 409, 410, 
 “AL, 413, 489 
 
 Bellerophon : : sop, eS, 
 i micromphalus a w=: 294, 
 
 5 stanvellensis ... 94, 158, 159, 
 
 186, 289 
 
 Belonostomus AC sis ee w. 504 
 5 Sweeti . 407, 412, 504 
 Beyrichia ... He ... 214 
 a varicosa ... 130, 137, 141, 181, 214 
 Billingsia alveoluris s a 53 
 Biziura vate ar ne eh weal |p (ODD 
 » exhumata ... bat 6c Ae 655 
 Brachalletes sas ee ant Oso 
 Palmeri ee ae oe O79 
 Brachyphyllum sie Set sae sou ahold) 
 * australe, var. crassum ... 3885 
 
 e crassum 353, 354, 363, 385 
 Bucania a oh are Se ANY) 
 x textilis 93, 94, 186, 290 
 Bulimus... Bie noe .. 646 
 “ Bairdii... Sa nite .. 646 
 
 A fibratus ... so sas .. = 646 
 Bulla ampulla ae ine 3 O90 
 Burrows ? a" 297 
 CALAMITES ... 91, 92, 93, 185, 186, 178 
 mr radiatus eae Loo 
 
 * varians ies 140, 141, 178, 188 
 
 sp. ind. Soe LOS 
 Campophyllum noe ati ane aa 60 
 -- Gregorii ... 44, 48, 6O 
 
 Canis dingo cat a oe sow OPP? 
 Casuarina oe Ge th ee o2e 
 Ceratochelys sthenurus ... 647, 650 
 Cardiocarpum & ae OOO 
 * australe ay, 353, 354, 363, 386 
 Ceratodus ... fe ein 646 
 x Fosteri ... Bia 50 ... 646 
 
 i Palmeri ede ea a 646 
 Cerithium ebininum Ae nh .. 642 
 Ceromya ... ee bof a 571 
 ra sp. ind. or BBA, 571 
 Chenomya ... tn Or sy) WARS! 
 " acuta iso, 185, 280 
 
 3 ? bowenensis ... 159, 185, 280 
 
 33 ? carinata Soo sth 159, 185, 279 
 
 + ? Etheridgei 84, 158, 159, 185, 279 
 
 Page. 
 
 Chelodina ae ate wa 048 
 an longicollis 6c .. «=»: 6 48 
 Chlamydosaurus —. vee ‘bs ies 1088 
 3 Bennettii vias .. 648 
 
 ie Kingi se 2048 
 Chonetes Soh Bee ACY 
 . australis ... 263 
 
 - cracowensis 
 
 a laguessiana 
 “ sp. ind. (a) 
 
 ” ” (0) 
 ”» 2 (c) 
 ” ” @) 
 
 Chronozoon .. 
 ry australe 
 Chosornis sae 
 33 preeteritus 
 Cinulia ae we 
 »,  Hochstetteri 
 Cladochonus Fi 
 * tenuicollis 
 Cladopora robusta... 
 Cleobis grandis 
 » recta 
 Codakia percrassa ... 
 Ceenites 
 Ee SDalud. 
 Conchotheca turgida 
 Conus glacus 
 Corbicella - 
 - P maranoana 
 Corbicula ve 
 _ australis 
 ‘, burrumensis 
 i nepeanensis 
 Corbula crassa 
 »  albuginosa 
 
 Cordaites sc 
 5 australis .., 
 Corimya... nee 
 * primula 
 “A Wilsoni 
 
 Crenatula ? Sena 
 Crioceras 
 
 5 australe . 409, 410, 411, 412, 413,499 
 
 . Edkinsi ... 411, 502 
 
 5 Jackii wu. 499 
 
 . irregulare “418, 409, 501 
 
 sp. ind. 411, 412, "502 
 
 Cristellaria ... Se ae em ww. 488 
 
 . acutauricularis, var. 
 
 longicostata 409, 435 
 
 x cultrata, var. radiata 409, 435 
 
 Crocodilus ... a0 : nee Boo. MY 
 
 x australis 606, 652 
 
 =. porosus... sO De 
 
 Cucullxa Pets ar 468, 565 
 
 ‘ss costata + se ee a) 
 
 a Hendersoni 411, 468 
 
 3 robusta ace 554, 565 
 
 Cultellus, sp ? a .. 695 
 
 Cunninghamites : pc x) | S80 
 
 a australis .., 353, 354, 363, Se 
 Cyathophyllum _... by sie ; 
 
 a Leichhardtii ... : 59 
 
 4 sp. ind. (a) Re 179, 201 
 
 i a te) és 179, 201 
 
 _ 92, 93, 94, 130, 137, 
 141, 158, 159, 183, 262 
 ey 
 
 92, 94, 130, 133, 
 
 138, 141, 183, 262 
 
 . 92, 93, 94, 183, 263 
 133, 138, 141, 183, 263 
 157, 159, 183, 264 
 ey: 
 
 682 
 
 657 
 
 657 
 
 484 
 
 “409, 410, 484 
 
 i ees 
 
 93, 179, 201 
 
 Tee 
 
 282 
 
 284, 
 
 569 
 
 56 
 
 43, 48, 56 
 
 os oe | RO 
 eu pa 5 Reames 
 pane ala 
 
 410, 471 
 
 319, 641 
 
 606, 641 
 
 312, 319 
 
 606, 641 
 
 695 
 
 695 
 
 198 * 
 
 83, 140, 141, 179, 198 
 
 = ni 
 410, 481 
 458, 459 
 499 
 
INDEX TO GENERA, ETC. 763 
 
 Page. 
 
 Cycadinocarpus ... aes dav) « O00 
 Cycadopteri is preacaats vides “as ne OOS 
 Cyclas nepeanensis.. ae He Be 641 
 Cyclopteris cuneata i ey 378 
 Cyclostigma “es : 135, 136, 197 
 ‘ australis 140, 141, 179, 197 
 
 sp. ind. 137, 141, 179, 197 
 Cypricardella ¥r ps S276 
 “f Jackii ae . 84, 184, 276 
 Cyprina 474, 568 
 
 ,  Olarkei 410, 412, 413, 414, 
 
 
 
 Page. 
 
 Dromaius patricius... Boe a OO 
 Dromornis ... mee oF 606, 658 
 of australis... .. 606, 658, 659 
 ECHIDNA ... oh <a og .. 663 
 a Oweni ... se aa ae OG. 
 Ramsayt.. aire aCe w. 668 
 Edmondia ae Fi ar Su 281 
 “6 obovate . sat 84, 185, 281 
 Entolium .... eae .. 264 
 
 474, 554, 555, 568 ee ie sp. ind. 130, 138, 141, 183, ee 
 noi quisetum ... aa A 
 »  expansa Ms 409, 474 E Platum 351, 354, 356, 362, 365 
 Cyrena atl bad + Be. vee GAL é rotiferum 351, 354, 356, 362, 364 
 + australis ie oo. ns Bar G41 Mathers a” if ; 347, 387 
 » _ nitida a ose ot a 693 = pacers ; 358, 354, 363, 387 
 Cystiphyllum re ew i ae 58 Taahicndsia’. E; iar SObK 
 4 americanum, var. aus¢ 4 SEAN g 130, 138 141, 183, 265 
 trale — . 43, 48,58 Euomphalus * he 285 
 Cytherea wore x see eee eee 473 sp. ind. Pe 92, 94, 185, 285 
 ” Clarkei 409, 474 Paowenin 669 
 »  ? Hudlestoni 411,473 grate meee a: 669 
 »  Moorei vs 411, 474 Sy robusta ea! Tien . 670 
 is ie av 409,473 Eurydesma A = iy ade Be ae, 
 3 ‘ cordata.., tes 185, 278 
 DASYURUS ... bs aa te 681 is mnacalud 185, 278 
 - viverrinus ve See POOL 
 Delphinula ... of of ww. 485 
 ? reflaoka be iz 410, 485 FAVOSITES ... te ioe ae Ane 50 
 Deltocyathus, sp. ind. a0 ae fone er » Goldfussi ve nee “ 50 
 Deltodus _... see Aan te Asks ” pean 43, 48, 50 
 3 australis ... - 93, 186,296 Fenestella te 157, 217 
 Deltopecten... R. $a ce eaoo ” densa... vn 217 
 * illawarrensis “ie 157, 159, 184, 269 ” fossula .., 83, 92, 94, 151, 159,181,217 
 Dendrocygna A = 655 % internata. 94, 181, 218 
 a validipinnis... 655 - multiporata 130, 137, 141, 181, 218 
 Dentalina a .. 435 be sp. ind. . sea 83, 89, 94, 181, 218 
 bs communis 409, 435 Fulica oo 658 
 Dentalium ee .. 4838 » prior . 658 
 a arcotinum 409, 483 » prior se 658 
 x lineatum 409, 483 
 re jongirostrum . 4 a.GOD GALAXEA ere we a Oo L 
 3 wollumbillaensis "410, 411, 483 Gallinula nas Sa Ae Aa MOA 
 Derbyia ti a sh PAS Fe peralata ... . 50 OO” 
 »  senilis pees led oO: 166, “177, 182 gee . strenuipes 43 Bet soe BY 
 Dicranophyllum tye Gastrochena < ai Sas 482 
 5 australicum 43, 47, 49, australis 410, 482 
 Dielasma .... se me eee 25) Gervilleia oan wae fh sae 409 
 _ cymboeformis 181, 225 . angusta ... Si te .. 409 
 * saccuius ... he 159, 182, 226 Glauconome we a Aon eS 
 is » var. hastata 938, 182, 226 a sp. ind. 93, 94, 181, 223 
 35 sp. ind. 93, 94, 182, 22:7 Gleichenia .., se aaa so eyes 
 Didymosorus ay if tie DOL ¥ bindrabunensis ... py 
 " ? gleichenioides 525, 554, 557 ~ lineata ... 352, 354, 362, 371 
 Dinornis ... sie ar : 662 Gleichenites bindrabunensis Si ODT. 
 » ?queenslandieg ... nee .. 662 7 odontopteroides et sos 
 <y. pe Owental.. i ae PE eOoS Glossopteris... 168, 169, 170, 171, 172, 
 Dinotherium australe a a ees, 6 668 174, 176, 198, 518, 519, 
 Dione bullata ee TBR « 695 520, 528, 5380, 554, 558 
 Diprotodon ... es _ 604, “607, 622 - ampla... 159, 178, 195 
 australis y 606, 607, 608, 668 ms Browniana 159,177, 179, 193, 300 
 : minor ... ae ee OOo s linearis Tate dss yap aly key 194 
 Discina ee 2S ae a we = 4G : moribunda ... TOOL 
 ‘,,  apicalis 409, 444 Glycimeris oe 478, 570 
 Dolium costatum 694, 698 e aramacensis 411, 479 
 Dosinia canaliculata a as’ St OUD 4 Maccoyi . 410,480 
 Dromaius ... ae aa — bon Meath a rugosa 410, 414, ‘478, 554, 555 
 »  gracilipes ue ae re eon " sulcata ... » Fr 554, 571 
 3 nove-hollandie .., ane rie OOL 5 Tater ean: ee ae .» 410 
 
764 
 Page. 
 
 Goniatites ... om ie el 
 i. micromphalus . kage: 186, 294 
 ~ planorbiformis 92, 93, 94, 186, 295 
 - Sp. ind. ies. 84, 88, 02, 0 186, 295 
 Goniomya sob .- 480 
 FS depressa.... 410, 480 
 Granatocrinus ee AS eee LO 
 35 Wachsmuthi 92, 94, 180, 210 
 Griffithides ... : aK 216 
 5 dubius ... 214 
 ¥ seminifera 2, 93, 94, 181, 216 
 Gyroceras ‘ 294. 
 PF dubius Soog eee ‘94, 294° 
 3 Philpi 44, 47, 48, 69 
 TIALMATURUS TEMPORALIS 613 
 ks stigmaticus... 613 
 Hamites 1h a .. 496 
 nf ? laqueus ... 411, 412, 496 
 Haploceras ... 4s 300 we 494 
 5 Daintreei 495 
 Fy Flindersi 494, 
 = Sutherlandi 4.96 
 Heliolites ae = 60 
 3 Daintreei 4A, 48, 61 
 5 Nicholsoni 44, 48, 63 
 3 plasmoporoides ... 44, 48, 62 
 - porosa ... 44, 47, 48, 61 
 Helix is 5a 610, 613, 645 
 »  Cunninghami ok ; 645 
 sy LNICOly 2 ves OLD 
 5  luloidea .. «=: 648 
 »,  Parsoni 645 
 »  splendidula .. ah o. 6493 
 ce FP var. strangeoides .. = 648 
 Whartoni .. 645 
 Homomy a sot 4.80 
 5 sp. ind. ... “410, 480 
 Hypsiprymnus Greyi 612 
 55 rufescens ... 612 
 ICHTHYOSAURUS : at a 505, 696 
 As australis... 394, 412,413,505 
 marathonensis ... 412,506 
 Inoceramus .. .. 462 
 * Carsoni- "394, 400, 412, 4138, 468 
 + Cripsianus AGS 
 : Cripsi . 406, 411, 465 
 elongatus "395, 412, 464 
 “f marathonensis 395, 412, 464 
 
 5 multiplicatus, var. 
 elongatus ... a6 395, 464 
 “i pernoides 395, 399, 411, 412, A464 
 = Sutherlandi ... 394, 400, 412, 
 
 KoALEMUS ... 
 
 + ingens ... 
 LmvVICARDIUM 
 % Brazieri 
 Lamna 
 
 »  appendiculata 
 »  Dayviesii 
 
 Lasiocladia ... wae 
 # ? Hindei 
 Leda australis ate eae 
 
 Leda pullata re vee 
 
 INDEX TO GENERA, ETC. 
 
 ” 413, 463, 464 
 
 671 
 671 
 
 . ~-496 
 
 413, 476 
 
 503 
 
 .. 503 
 
 413, 508 
 
 ee ae) 
 
 ‘98, 179,199 
 hee AGS 
 Th. er et: 
 
 
 
 
 
 Page. 
 Lepidodendron _.... pr eeles 
 x australe aor 92, 98, 115, 121, 
 129, 130, 135, 137, 
 140, 141, 179, 196 
 “A nothum ... ee tO 
 “ veltheimianum | 129, 140, 141, 
 179, 196 
 :. sp. ind. -137, 140, 141, 179, 197 
 Lepralia .... one we AAT 
 x oolitica Ae .409, 441 
 Leptoria, sp. ind. ... 06 556 re esa 
 Leptosiagon.,.. te Git at a 674 
 , gracilis sce nhc << OE 
 Lima ae 2M, 447, 562 
 His braamburiensis 409, 44:7 
 » Gordon 409, 447 
 » ? multistriata 409, 448 
 », Randsi 554, 562 
 sp. ind. eae ‘ae 554, 563 
 Limaw fibratus Sst tes ane «at 9) 046 
 Limnxa ... Agr ae BS w. 644 
 4 rUMosa Pe 606, 644: 
 cs yinosa 606, 644 
 Lingula aaa 264, 44.4: 
 % mytiloides... 88, 183, 264. 
 » _ Ovalis _ 408, 409, 444. 
 subovalis ... an 409, 444 
 Lithophaps ... ob ne 2g 2+ 8606 
 a ulnaris oi sie OO 
 Loxonema ... At eae ity, sels 
 ‘3 sp. ind.... 92, 94, 185, 285 
 Luciella ee =, Sue 3 e238 
 + Gray 93, 94, 186, 288 
 Lucina anomala ... Ae . 450 
 ¥ 2? australis ... its es RAY co oll 
 Lutraria... see ee Rrpe  ay es 
 - sprind. 5. sep 554, 572 
 MAccoYELLA me ‘s 451, 503 
 z Barklyi 410, 413, 414, 453, 
 454, 455, 459, 460, 555 
 
 by 5 var. marice- 
 buriensis 458, 554, 563 
 . corbiensis .,. 410, 414, 454, 458, 
 554, 555, 563 
 * reflecta 410, 414, 452, 454, 
 457, 458, 554, 555, 563 
 3 substriata .., 410, 414, 454, 458, 
 460, 554, 555, 563 
 cs umbonalis ... 410, 414, 454, 458, 
 459, 564, 556, 563 
 Macrocallista $s i33 we = 475 
 4 ? plana “410, 413,476 
 Macropus ... Gs a : 672 
 -* affinis ... _ aye ee Gy: 
 5 Ajax oe; sh a 674 
 re robustus Sas ee we 674 
 ss itanvaeess as AS 2 OTS 
 sp. ind. . ans ee pee YE 
 Macroteniopteris is ma : 376 
 As crassinervis B56, 368, 376 
 5% lata Bab 4 No 361 
 . wianamatte ... 352, 354, 
 ' 368, 376 
 - sp. ind.... 363, 377 
 Mactra a a hes OL 
 * trigonalis ie He aoa 411, 481 
 
 peesp sind Fak nt a OOo 
 
INDEX TO GENERA, ETC. 765 
 Page. Page. 
 Martinia aa ave 236, 237 Mytilus... if vee owe ve «= 466 
 +9 ? productoides . 88, 92,94, 182, 236 50 SBigshyiv. 3. eee vee vapeele 
 GF subradiata ‘ 84, 158 A) anileacusmmerss ..» 409, 410, 413, 467 
 Martiniopsis a AS n eee 230 5» ingens oe : wor 411, 467 
 5 Darwinii 95, 157, 159, 182, 240 - linguloides nos ae k 409 
 . subradiata 159, 182, 288 » planus soe we = 466 
 Fe 3 var. Koninckii ... 239 »  Tugocostatus oe 409, 410, 466 
 es ; var. Mor- »  Scoulari ae * iin) $409 
 risii 88,182, 239,240 »  Tenison-Woodsi 410, 466 
 rf x var. trans- 
 
 versa ... 239 NASSA LIQUIJARENSIS nas as BO GEES 
 Mastodontoid Te dada a. 268 ; Pe spainds ae seu GOOD 
 Megalania ... : 647, 649, 650, 651 Natica , nee 485, 573 
 HU prisca 649, 650 »  dackii 413, 486 
 i prisca 647 » lineata 409, 485 
 Meiolania ... ve noc, ot vp »  oOrnatissima ... 410, 486 
 ‘A minor 647, 650 55 plumbea : . 648 
 FA Owenii ... 647, 651 »  variabilis ; “409, 410, 414, 
 5 platyceps the 647, 650 485, 554, 555, 573 
 Melania ies ae fe 642 »  variata : : age whet 
 ms arca ; one 606, 642 sp. ind. 485 
 * balonensis... 606, 642 Naticopsis ei ; Sie, aeiee: 
 »  clayus am 4 Oe > harpeeformis , .. 93, 94, 185, 284 
 denisoniensis 606, 642 variata 130, 188, TAL, 185, 285 
 3 moesta 606, 642 5 SYOH MAB, oc 130, 138, 141, 185, 285 
 5 onca A 606, 642 Nautilus a Nee e 292, 502 
 » pagoda 606, 642 HK: ? ammonitiformis 93, 94, 186, 292 
 - subimbricata 606 5 Hendersoni 411, 412, 502 
 sp. ind. 606 a sp. ind. 93, 94, 186 
 Meleagrina .. Be (Oe Necrastur 354 
 Meleagr inella 453, 482 a alacer 354 
 Melosira arenaria ... 330 Neritina gagates 694 
 Merismopteria ne Se eg Notiosaurus AA 651 
 % macroptera _ 159, 184, 271 ms dentatus 651 
 Mesoblastus * 5 walls, Notochelone oe OOO 
 oe ? australis 93, 159, 180, 210 3 costata | 396, 412, 505 
 Mesostigmodera_... Ant MeL OO L Notochelys costata . oe 396, 505 
 lee ; 353, 354, 363, 387 Notoelephas i ee wf 683 
 Metapteryx .. ; eLOO2 7 australis ees 5 tao, Kehes3 
 =f bifrons.. a 662 Nototherium be , 606, 607 
 Micraster 4 wx, HY) mn dunense OO? 
 45 Sweeti Be 554, 559 =, inerme . 667 
 Mitra, sp.? ... i Oue of Mitchelli ae LOOT 
 Modiola be 468 -| Nucula 469, 565 
 »  linguloides... OT, » australis 410, 469 
 » unica 410, 468 COO pert 410, 469 
 Modiomorpha Ser a ee » gigantea : 554, 566 
 ss Daintreei 88, 184, 272 »  quadrata 406, 409, 411, 414, 
 “p mytiliformis 157, 158, 469, 554, 555, 565 
 ° 159, 184, 273 » truncata cai 409, 410, 469 
 Monotis Barklyi : 4.55 sy toh eavell “6 F 93, 94, 138, 184, 
 Monticulipora ee (2, 274, 406, 411, 470 
 ” sp. ind, 89, 180, 202 Nuculana ... not “ i 276, 566 
 Mourlonia ... ae ne eS 4 Randsi . ae 554, 566 
 = ? coniformis i 158, 159, 185, 287 5 sp. ind. 130, 188, 141, 184, 275 
 ‘e Strzeleckiana 92, 94, 185, 287 Nyroca 655 
 Murchisonia : e289 5 australis 656 
 Me carinata 93, 94, 186, 289 or reclusa 656 
 “ sp. ind. (a) 93, 94, 186, 289 » robusta 655 
 
 » » (0) 93, 94, 186, 289 
 » x. | (e) 93, 94, 186, 227 Odontopteris OG Babes 368 
 Mya McCoyi 1 w. 480 Oliva ispidula : bis wv. 695 
 Myacites McCoyi ... ae 409 5, Jlepida... “he wea aw » 69D 
 » TUYOSA st ... 409 a neostina a6 ee ... 695 
 Myophoria ... : 470 » sidelia,.. eee vue pa aun CO5 
 Myriolithes .. 225 BPA. tise se oe pp 8219) 
 * queenslandensis 89, 92, 94, Orbipora ? Waageni acs, on sou, NTs 
 181, 225 Ornithorhynchus 663 
 Mytilops.... tie +r ese ala . agilis vee vw» 668 
 »  ? corrugata a 93, 94, 184, 272 Orthis 244, 
 soe COB Ate «7 va venuit OAs, 184, 272 » australis 92, 93, 182, 245 
 
766 
 
 Orthis resupinata ... 
 
 INDEX TO GENERA, ETC. 
 
 Page. 
 88, 92, 93, 130, 
 137, 141, 182, 244 
 
 Orthoceras ... Soe eee 298 
 nA sp. ind. ... B4, 93, 94, 130, 138, 
 141, 157, 159 , 186, 293 
 Orthotetes ; é : 68 
 As concentrica A, 47, 68 
 - crenistria He ie 68 
 i Mi var. senilis ... . 246 
 ‘ wnbraculum 44, 47, 68 
 Osphranter at ee 
 . Cooperi 674 
 5; Gouldi Son ws 
 Ostrea : 445, 531, 536, 561, 640 
 » mordax 3 640 
 »  pes-tigris ... 640 
 »  vesiculosa 412, 445 
 Resp ands * BBA, 561 
 Otodus appendiculatus . 307, 413, 503 
 Otozamites ... soo toll 
 Ms Mandeslohi 323, 354, ee 381 
 7 sp. ind. ; 2, 318 
 Owenia grata ’ 669 
 Oxytoma 3 . 448 
 a rockwoodensis _ 411, 412,448 
 s ? simplex 410, 449 
 PACHYDOMUS : 282 
 E globosus _ 159, 185, 282 
 Pachypora ... ae e 51 
 & mericionalis _ 43, 47, 48, 51 
 Pachysiagon : aoc poe heiress 
 BS Ferragus 75 
 BA Otuel 075 
 Parallelodon XK: we DTA 
 s costellata 84, 274 
 Paleomeera.. 478, 570 
 es marieburiensis iE 554, 570 
 Sr sp. ind. 411, 478, 554, 570 
 Palzoniscus ot 186, 188, 140, 141 
 4 Randsi sf 186, 296 
 Paleopelargus . 354 
 - nobilis 354 
 Palorchestes sy 675 
 4 azael .,. 675 
 Pallimnarchus 5 652 
 - pollens AOD 
 Panopea 478, 570 
 TUgOsSa 478 
 5 sulcata ee OL 
 Pecopteris australis 316, 360 
 , gleichenoides 557 
 a odontopteroides 368 
 Pecten ae = 445 
 »  equilineatus 409, 445 
 5  comptus 266 
 »  fimbriatus .. 445 
 »  limeforiis ... bi 266 
 »  Moorei 409, 44.5 
 
 »  nove-guinese 
 »  psila 
 »  socialis , 4 
 e subquinquelineatus 
 sp. ind. 
 Pelicanus ae 
 3 proavus ... 
 Pentacrinus.. 
 Fe australis 
 Pentamerus.. eon 
 5 brevirostris ans 
 Perameles nasuta ... 
 
 a 692, 698 
 .. 409, 411, 446 
 409, 413, 446 
 wah 266 
 2, 446, 695 
 354 
 
 354 
 
 .» 439 
 “409, 410, 489 
 Be 67 
 
 411, 41 
 
 4A, 47, 67 
 soo LOUUB 
 
 
 
 Perna 
 
 » gigantea 
 Peronella decagonalis 
 Petrogale penicillata 
 
 Phalanger a 
 = procuscus 
 Phalangista canina 
 Phascolagus 
 5 altus 
 Phascolomys es is 
 x angustidens ... 
 a GJigas... 
 nS magnus 
 & medius 
 * Mitchelli 
 5 parvus re 
 a platyrhinus ... 
 f pliocenus 
 rr Thomsoni 
 Phascolonus 3 Bi 
 A gigas ... ea 
 Phillipsia 
 
 *, dubia 93, 94, 130, 
 ye Woodwar di 
 Fe sp. ind. 
 Phlebopteris 
 fs alethopteroides 
 Phyllopteris 
 i Feistmanteli... 
 Phyllotheca : 
 x australis 
 i carnosa 
 a sp. ind. 
 Physa see 
 » truncata 
 Pinna Re 
 » australis 
 Pe epalnds 
 Placuna 
 F sp. ind, 
 Planorbulina oad 
 = lobatula 
 5 Ungeriana 
 Platalea ae 
 a subtenuis .. 
 Platyceps Wilkinsoni 
 Platycrinus ... So 
 5 CREDUL Kat 
 Platyschisma 
 a acutus 
 * rotundata 
 
 Plesiosaurus.. 
 L macrospondyl lus 
 Fs Sutherlandi .. 
 
 Pleurophorus 
 Randsi 
 Pleurotomari 1a 
 Ss carinata 
 “ Cliftoni 
 Plotus es 
 5  parvus 
 Podozamites ae 
 fe Barklyi 
 * ellipticus 
 5 Kidstoni 
 : lanceolatus 
 55 sp. ind. 
 
 Polymorphina vse 
 
 Page. 
 
 pee) 
 
 410, 462 
 
 692 
 
 613 
 
 670 
 
 670 
 
 613 
 
 676 
 
 Meee. 
 ... 606, 607, 664 
 605 
 666 
 
 664 
 
 .. 664 
 
 605, 664 
 
 665 
 
 665 
 
 622 
 
 665 
 
 666 
 
 666 
 
 ve 214 
 
 137, 141, 181, 214 
 92, 94, 181, 215 
 
 . 92, 93, 94, 181, 215 
 
 I 378 
 
 352, "854, 363, 378 
 ‘ 378, 518 
 354, 356, 362, 375 
 ane 168, 365 
 177, 178, 189 
 351, 354, 362, 8365 
 351, 354, 362, 865 
 “ae 644 
 
 606, 644 
 
 fe HOD 465 
 he a 466 
 “418, 465 
 
 a: 562 
 
 554, 562 
 
 436 
 
 409, 436 
 
 409, 436 
 
 354 
 
 3854 
 
 860 
 
 Ma Bi 208 
 159, 180, 208 
 
 or 286 
 
 94, 185, 286 
 93, 94, 158, 
 
 159, 185, 286 
 B08, 509 
 394, 413, 508 
 394, 411, 412, 
 413, 508 
 
 ads ees 
 WES 71S4n 27a 
 aks bon 287 
 
 . 84,185, 287 
 410, 484 
 
 656 
 
 656 
 
 Sule 
 
 360 
 
 ; 360 
 
 “311, 312, 317 
 352, 354, 363, 380 
 311, 312, 318, 352 
 354, 363, 380 
 
 436 
 
 nee oor 
 
INDEX TO GENERA, ETC. 
 
 Page. 
 Polymorphina gibba 409, 436 
 oe lactea Ae 409, 436 
 Polypora... a ay aie kh 
 te ? Smithii ... 83, 92, 93, 94, 181, 219 
 Porcellia ... we ... 290 
 * Pearsi : 93, 94, 1380, 138, 
 “14, 158, 159, ee 290 
 Porphyrio ... a 657 
 As Mackintoshi_ ... a ee ODF. 
 Re ? reperta one ee OUT 
 Potamides ... es ane eos ws | 642 
 a ebininus at “fe ee 642 
 Poteriocrinus of Re See 209 
 a crassus son ABE “180, 209 
 ‘ Smithii ag 93, 180, 209 
 Procherus ... es ane 682 
 - celer .... toe 2s ... * 682 
 Procoptodon ee ey Wes POLO 
 rp Goliah site aes OVO 
 a pusio don Act coe O70 
 BS rapha ve re soe RE 
 Productus ... tie me 247 
 _ brachytherus ... 87, ‘88, 92, 98, 94,, 
 159, 177, 183, 248 
 A: Clarke 2OS 
 cora . 84, 92, 94, 157, 159, 183, 248 
 
 e longispinus 93, 94, 183, 255 
 
 o semireticulatus 88, 92, 94, 183, 255 
 iy subquadratus 92, 4, 9, 159, 252 
 i sp. ind. (a) ; 87, 255 
 > eed (G) 92, 94, 255 
 A ey Ge 92, 9A, 256 
 ae (cl) ; 93, 94, 256 
 3 . ite) 158, 256 
 ” ” (f) 99, 257 
 Progura os a Soo a s 656 
 » gallinacea ne ee Oot 
 Protemnodon An hos cos oe OFT 
 Pe anak ... uae fs sc5 9 OWE 
 5 anteeus es sa ee OL 7 
 iP mimas aS Bon cee Or d, 
 x Gores aCe ae a O18 
 i Reechus wee ae Ee Oe 
 Protoretepora we Oko 
 i ampla 83. 92, 94, 151, 181, 221 
 * » var. Konincki stat 159, 
 181, 222 
 e » var. Woodsi... 159, 181, 222 
 Pseudavicula we 449, 563 
 a ? alata 554, 563 
 y anomala 410, 450 
 a australis nee ae 410, 451 
 Pseudochirus ms * es ao, Soya 
 a ?notabilis ... he AL 
 Pterinea macroptera na a nee | meatal 
 Pterinopecten os ae oh, rere 
 _ Deyisii 93, 94, 184, 270 
 Pterophyllum _" be el dant! 
 4 abnorme : 358, 354, 363, 381 
 - sp. ind.) 353; 354, 356, 363, 382 
 Ptilophyllum 4g da ge eso 
 “aes eo 363, 382 
 Pupina Coxi : ve ats 643 
 # meridionalis Be Sc . 643 
 RANELLA ALBIVARICOSA ... aoe to a 695 
 Reticularia ... Aes Se 235 
 
 * lineata ... oe 93, 94, 182, 235 
 
 i Urei 130, 137, 141, 182, 235 
 Retzia me on Ais . 242 
 »  ? lilymerensis crs 92, 94, 152, 242 
 
 Retzia radialis 
 
 Rhombopora ww. 224 
 3 laxa ‘83, 92, 94, 181, 224 
 Rhynchonella 244, 443, 536, 560 
 BS croydonensis 564, 560 
 pleurodon ... 92, 94, 133, 137, 
 
 141, 182, 244 
 
 , primipilaris -. 44,47, 67 
 
 % rustica 409, 443 
 
 ‘* solitaria 409, 444 
 
 3 variabilis we | 408 
 
 s sp. ind. : 244. 
 Rocellaria ... re ve 319 
 a ee 312, 319 . 
 Romingeria . awe a8 56 
 53 ? Foordi- 43, 48,56 
 SAGENOPTERIS oie Pos SUEY if 
 “ ? cuneata ... 352, 354, 363, 378 
 
 4 rhoifolia ... 323, 352, 354, 
 
 "363, 377 
 
 Sanguinolites 4 eco 
 concentrica ... . 84, 185, 281 
 
 Sarcophilus ... “on Aetshll 
 as laniarius 680 
 
 “ prior 681 
 Sceparnodon : 681 
 Es Ramsayi 681 
 Schloenbachia 493 
 i inflatus 493 
 Sequoiites ee .. 884 
 % australis 355, 356, 363, 384 
 Serpula Ge .. 440 
 = intestinalis . 408, 409, 440 
 Siphonaria ... eee Be Es 
 Samwelli 554,573 
 Solemya_... i oe 24D 
 »  Edelfelti “159, 184, 275 
 Sphenopteris : of 169, 190, 314 
 ap Bailiana 351, 354, 362, 366 
 
 rr crebra .. 177, 178,190 
 
 Sphenopteris elongata 
 
 767 
 
 Page. 
 130, 187, 141, 182, 242 
 
 367 
 
 3 flabellifolia ... 311, 312, 314 
 
 . Fr var.erecta 311,312,314 
 .s flexuosa 177, 178, 190 
 
 a lobifolia 177, 178, 190 
 Spirifera ee FA eee 227 
 Sh bicarinata : 88, 92, 94, 130, 183, 
 137, 144, 182, 234 
 
 ig Clarkei ae 159, 182, 229 
 as conyoluta ... 154, 182, 229 
 - curvata 44, 47, 64 
 S dubia .. 83, 182, 231 
 5 euryglossa 65 ne ‘44, 47, 65 
 ap lata 95, 157, 159, 182, 229 
 . pinguis a 93, 94. 182, 233 
 * Stokesii 83, 95, 159, 182, 232 
 s striata . 159, 182, 227 
 . Strzeleckii 157, 159, 182, 234 
 a tasmaniensis Ae 159, 182, 232 
 _ trigonalis woos 94, 159, 182, 230 
 . e var. acuta 83, 230 
 :. * var. bisuleata eee 2o0) 
 > a var. crassa 92, 94, 230 
 - ¥ var. Strzeleckii 83, 182 
 7 vespertilio 83, 92, 94, 182, 228 
 n sp. ind. (a) 03, 94, 157, 228 
 %9 » (0) wee + 231 
 Spiriferina ... ify “i w= 234 
 nf duodecincostata 137, 157, 182, 234 
 
 or sp. ind..., ese 
 
 130, 141, 182, 235 
 
768 INDEX TO GENERA, ETC. 
 
 Page. 
 
 Spondylostrobus_ ... es ae eco 
 Sporangia ... AAC ae a8 Se OL. 
 Stenopora ... use os eee 
 3 australis Rae "159, 180, 202 
 
 i gimpiensis ; 83, 180, 206 
 
 s Jackii 151, 159, 180, 205 
 
 RS Leichhardti 151, 159, 180, 204 
 
 3 ovata... ae .. 1202 
 
 Stephanoceras 5G: ac <p sop SLE 
 
 Sthenomerus oa eh ae OLS 
 
 * Charon sh hes ee OLS 
 
 Sthenurus ... swe str sa OTS 
 
 as IA TIAS aur ee Be ie Soo cys! 
 
 “4 Brehus ... ia wee OLS: 
 
 Stigmaria ... a 3 weae AOS 
 
 * sp. ind. ... 140, 141, 179, 197 
 
 Streptorhynchus crenistria 60 Shc 68 
 
 fe 5 var.senilis ... 246 
 
 a Davidsoni xB w= 455 
 
 umbraculum  ... nee 68 
 
 Striatopora .. Foe sn : 55 
 
 Bi uniseptata 43, 47,55 
 
 Stringocephalus _... 5 aie 67 
 
 " sp. ind. ... Sis 4A, 47, th 
 Stromatopora : ses ms 
 
 Ms sp ind. “48, 47, 48, 49 
 
 Strombus canarium ote a aeOOD: 
 
 Campbelli aia Ho OS 
 
 Strophalosia sae ma ZS 
 
 2 Clarkei 151, 158, 159, 183, 258 
 
 . Gerardi ... 158,159, 183, 260 
 
 “ Woodsi 505 aint Migs Atte: 
 
 Strophomena oe - a we 245 
 
 # rhomboidalis, var. 
 
 analoga 84, 93, 94, 180, 
 
 137, 141, 188, 245 
 
 Synaptodon ... ay ae ca (EO 
 
 a sevorum By ee me 080 
 
 T#NIOPTERIS a on se 371, 518 
 
 - Carruthersi ... .. 852, 354, 356, 
 
 362, 374 
 
 u Daintreei_ ... 311, 313, 317, 323, 
 
 352, 354, 356, 359, 
 
 360, 362, 371 
 
 3 tasmanica + sop el 
 
 Tancredia ... Fee +e af eed 
 
 > P plana . 410, 477 
 
 - sp. ind. ., ee 410, 478 
 
 Taphetus... 6 be 5B ageegOOS 
 
 Es brachialis Rat aes PODS 
 
 Taxites kar Aric Ba . 884 
 
 »  medius 353, 354, 363, 384 
 
 Tellina foliacea ... we 695 
 
 »  McAndrewi ae ep Pe OOo: 
 
 » pinguis one Ae ase OUD 
 
 »  scalpellum ... Ads ae LOCO 
 
 5 eeapectabilis —.. sae as ae eb: 
 
 ay ajekbey a he a co OOO 
 
 Terebra straminea ... dite bap Bog Leos) 
 
 Terebratella xe ies os 442 
 
 Davidsoni 409, 442, 
 
 Tercbratula cymbeeformis .. 159, 225 
 
 Fi sacculus _ 159, 226 
 
 Teredo oe ace is Aa 5, OYA 
 
 Bp ond: 554, 572 
 
 
 
 Page. 
 
 Temnechinus Macleayana... fen ey Cols! 
 Teuthis : ee 2 ABs 
 ee ED. nds 50 410, 487 
 Thalassina ... ds Ai ees Lae Ope 
 Emerii ... ois ate Ren) fabs, 
 Thinnfeldia .. ry: ns ea ao) Oe 
 3 cr aacineryis ae et OOS 
 
 5 media ... “311, 312, 315, 
 352, 354, 362, 369 
 
 “ odontopteroides 851, 354, 
 
 357, 362, 368 
 
 y Ae var. fal- 352, 354, 
 
 cata 362, 369 
 
 a subtrigona we one ae sin! 
 Thylacinus ... ee ic 500 -- 680 
 os speleeus a Jeo 680 
 Thylacoleo ... os Fs .. 606, aie oe 
 
 3 carnifex % : ae 
 
 Thracia Wilsoni ... ue ioe ase ist 
 Trachypora .. ae ae ae et 55 
 fe sp. ‘ind. . 43, 47, 55 
 Tribonysc., Aor Mae ioe ae) OOS 
 _ effluxus ... se MBs OOS 
 Trichomanites ey ate Bee ley 
 ig elongata Bball 354, 362, 367 
 
 y laxum 811, 312, 315, 
 
 351, 354, 362, 367 
 
 - spinifolia ... —... 851, 854, 362 
 Triclis BE Ace Bee aa OLS 
 * oscillans  ... we vA vas ee 
 Triccelocrinus ose ae wae pale 
 - Carpenteri ... 93, 94, mis, 212 
 Trigonia... os tae ee 470, 567 
 e lineata ... 409, 410, 470, 567 
 
 “4 mesembria es 411,470 
 
 i nasuta 409, 554, 567 
 
 a APs ttc sco 411, 471, 554, 567 
 UNICARDIUM we : a 472, 569 
 - # Etheridgei . 554, 569 
 
 ys Meeki a 413, 472, 
 
 Unio Se see Are ae 388, 468 
 » eyrensis ... 858, 354, 363, 389 
 
 »» ipsviciensis ... 358, 354, 363, 388 
 esp: ands Nar ae ... 889, 412, 468 
 Uroetus br achialis Aen se Gos 
 VAGINULINA ae Be ae w. 485 
 = striata : Le 409, 435 
 Varanus... ne sys nae Zn ee Ook 
 - dirus ® re Bi sy Letaile 
 
 ~ emeritus ... we oa fee KL 
 CS CUS es ac we 649 
 Venus (Chione) ealophylla are Baie Psy! 
 < imbricata ., sine Bae tls 
 
 Voluta anticingulata a on 694, 697 
 macroperta 694, 697 
 XENORHYNCHUS ... nae ee (ODS 
 55 nanus .., a OOS 
 YVANIA oe Sn aed ee tote: 
 . s Koninckiils.. 93, 94, 186, 288 
 ZAMITES LONGIFOLIA 356 ae OOO 
 Zaphrentis ... sh 500 x sae 
 
 "93, 179, 200 
 
 i; profunda ee 
 
 By Authority: James C. Brat, Government Printer, William street, Brisbane. 
 

 

 
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