THE UNIVERSITY 
 
 OF ILLINOIS ^ - 
 LIBRARY 
 
 557 
 
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 no.62~ 65. 
 
 
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Digitized by the Internet Archive 
 in 2016 
 
 https://archive.org/details/greenstoneschistOOwill 
 
THE 
 
 MISCELLANEOUS DOCUMENTS 
 
 OP THE 
 
 HOUSE OF REPRESENTATIVES 
 
 FOR THE 
 
 SECOND SESSION OF THE FIFTY-FIRST CONGRESS. 
 
 18 9 0 -’ 91 . 
 
 WITH INDEX. 
 
 IN SIXTEEN VOLUMES. 
 
 WASHINGTON: 
 
 GOVERNMENT PRINTING OFFICE. 
 1891 . 
 
 I 
 

6 5 7 
 Xfc> 
 
 h' 0 & -i, - (p ^ 
 
 /V uJ \C 
 
 vV 
 
 557 
 
 X*= 
 
 /Vo & ?L~ 6 ^T 
 
 INDEX TO HOUSE MISCELLANEOUS DOCUMENTS. 
 
 CONTENTS OF THE VOLUMES. 
 
 Vol. l..Nos. 1 to 127, inclusive, except Nos. 12, 13, 
 14, 76, 77,78,108.- 
 Vol. 2.. No. 12. 
 
 Vol. 3.. No. 13. 
 
 Vol. 4.. No. 14. 
 
 Vol. 5.. No. 76. 
 
 Vol. 6.. No. 77. 
 
 Vol. 7.. No. 78. • 
 
 Vol. 8.. No. 108, 133,134,135 
 
 Vol. 9.. No. 128. 
 
 Vol. 10.. No. 129, pt. 1. 
 Vol. 11.. No. 129, pt. 2. 
 Vol. 12.. No. 130. 
 
 Vol. 13.. No. 131. 
 
 Vol. 14.. No. 132. 
 
 Vol. 15.. No. 136. 
 
 Vol. 16.. No. 137. 
 
 Subjects. 
 
 No. 
 
 Vol. 
 
 A. 
 
 Alexander, John W., administrator, report of Court of Claimson case of. 
 
 Anacostia and Potomac River Railroad, annual report of 
 
 Army, retired officers, resolution relative to in the civil service 
 
 Astronomical observations for 1886 
 
 Ayres, Asa B., et al., resolution to refer claims to Court of Claims 
 
 121 
 
 84 
 
 92 
 
 132 
 
 120 
 
 B. 
 
 Bailey, John C., administrator, report of Court of Claims on case of... 
 
 Barnett, J. C., administrator, report, of Court of Claims on case of 
 
 Barnett, Julia, resolution to refer claim to Court of Claims 
 
 Beachley, Ezra and Jonas, executors, report of Court of Claims on case 
 
 of 
 
 Boarman, Aleck, resolution to impeach 
 
 Brashear, Martha, administratrix, report of Court of Claims on case of. 
 
 Brown, F. W., administrator, report of Court of Claims on case of 
 
 Bruen, Capt. John T., resolution to refer claim to Court of Claims 
 
 118 
 
 71 
 
 90 
 
 51 
 
 117 
 
 97 
 16 
 
 98 
 
 C. 
 
 Calhoon, Clement, report of Court of Claims on case of 
 
 Canter, Isaac W., administrator, report of Court of Claims on case of .. 
 Capitol, North O street and South Washington Railroad Company, an- 
 nual report of 
 
 Caruth, Thomas, report of Court of Claims on case of 
 
 Chapin, Virginius P., report of Court of Claims on case of 
 
 Chapman, William H., report of Court of Claims on case of 
 
 Christian Church, of Marshall, Mo., resolution to refer claim to Court of 
 
 Claims 
 
 Claims, report of Treasury Department in relation to certain specified 
 
 in House Ex. Doc. No. 314, Fifty-first Congress, first session 
 
 Clark, Samuel I., assignee, report of Court of Claims on case of 
 
 Clem, Anderson A., report of Court of Claims on case of 
 
 Clerk of the House of Representatives : 
 
 Annual report of the clerks and employes in the House 
 
 Report on inventory of public property in possession of 
 
 Commissioner of Fish and Fisheries, expenditures by the 
 
 Congressional Library, report on construction of building for the 
 
 Conrad, Ebenezer J. et al., report of Court of Claims on case of 
 
 Conrad, John D., report of Court of Claims on case of 
 
 21 
 
 62 
 
 95 
 
 60 
 
 81 
 
 42 
 
 126 
 
 22 
 
 65 
 
 67 
 
 6 
 
 10 
 
 5 
 
 4 
 
 17 
 
 28 
 
 in 
 
 1 
 
 1 
 
 1 
 
 14 
 
 1 
 
 l 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 l 
 
 •1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 N0\6 \ 
 
IV 
 
 INDEX TO HOUSE MISCELLANEOUS DOCUMENTS. 
 
 Subject. 
 
 Constitution of the United States, relating to violation of the four- 
 teenth amendment to the 
 
 Consular reports 
 
 Contested-election cases, digest of 
 
 Contested-election cases, print digest of, in the Fifty-first Congress ... 
 Court of Claims : 
 
 Report of the, on judgments of the - 
 
 Report of dismissed cases by the 
 
 Creek Indians, protest of delegates of the, in relation to jurisdiction of 
 
 Federal courts in Indian Territory 
 
 Crockett, John T., report of Court of Claims on case of 
 
 No. 
 
 Vol. 
 
 122 1 
 
 128 9 
 
 137 16 
 
 105 1 
 
 11 1 
 
 40 1 
 
 104 1 
 
 45 1 
 
 D. 
 
 Daub, Ezra, report of Court of Claims on case of 
 
 Deck, George, report of Court of Claims on case of 
 
 De Loach, Claiborne, estate of, resolution to refer claim to Court of 
 
 Claims 
 
 Department of Labor, expenditures in the 
 
 District of Columbia, Zoological Park Commission, final report of 
 
 Donato, Relate A. et al., resolution to refer claims to Court of Claims. . 
 Doorkeeper, House of Representatives : 
 
 Report of property in possession of..... 
 
 Report of sale of waste paper 
 
 24 
 
 54 
 
 101 
 
 9 
 
 93 
 
 115 
 
 8 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 E. 
 
 Eckington and Soldiers’ Home Railway Company, annual report of 
 
 Elkins, William A., report of Court of Claims on case of 
 
 Ely, Robert M. et al., resolution to refer claims to Court of Claims 
 
 Embry. W. J., executor, report of Court of Claims on case of 
 
 85 
 
 48 
 
 106 
 
 64 
 
 F. 
 
 Fairex, Mathilde M., administratrix, report of Court of Claims on 
 
 case of.. 
 
 Fish Bulletin, report for 1889 
 
 Fish and Fisheries, report of the Commissioner of, on expenditures 
 
 Fish hatchery, resolution relative to, in northern New York... 
 
 Fisher, Isaac, et al., resolution to refer claims of to Court of Claims .... 
 
 Fisher, John, et al., resolution to refer claims to Court of Claims 
 
 Flagg, Robert S. and Thomas G., executors, report of Court of Claims 
 
 on case of 
 
 Flower, Mary J., report of Court of Claims on case of 
 
 Fort Brown military reservation, relation to rent of 
 
 Freedmans’ Savings and Trust Company, annual report of the commis- 
 sioner for 1890 
 
 35 
 
 131 
 
 5 
 
 46 
 
 110 
 
 113 
 
 61 
 
 59 
 
 100 
 
 26 
 
 G. 
 
 Galloway, Thomas S., administrator, report of Court of Claims on case 
 
 of 
 
 Gay, Hon, Edward J., deceased, eulogies upou 
 
 Geological Survey, bulletons 62 to 65 
 
 Georgetown Barge, Dock, Elevator and Railway Company, report of 
 
 names of stockholders and condition of 
 
 Georgetown and Tennallytown Railway Company, annual report of.. 
 Gillilan, Ruth S., administratrix, report of Court of Claims onoase of.. 
 
 Gray, George L., report of Court of Claims on case of 
 
 - i • 
 
 H. 
 
 37 
 
 108 
 
 136 
 
 87 
 
 86 
 
 63 
 
 79 
 
 Heberlein, August, estate of, resolution to refer claim to Court of 
 
 Claims 
 
 Hightower, Thomas, report of Court of Claims on 'case of.. 
 
 Horse Diseases, report relating to 
 
 107 
 
 66 
 
 130 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 13 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 8 
 
 15 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 12 
 
INDEX TO HOUSE MISCELLANEOUS DOCUMENTS. 
 
 V 
 
 Subject. 
 
 No. 
 
 House of Representatives : 
 
 Clerk of (Hon. Edward McPherson), annual report of clerks and 
 
 employ 6 of the 
 
 report on public property in pos- 
 session of 
 
 Committees, list of standing and select 
 
 Doorkeeper, report of property, 
 
 report of sale of waste paper 
 
 Galleries of the, removal of partition and, on the south side of 
 
 Members, list of .. 
 
 alphabetical list of i 
 
 Special messengers, resolution to pay 
 
 Ho wery, Lewis, report of Court of Claims on case of 
 
 6 
 
 10 
 
 2 
 
 7 
 
 8 
 
 125 
 
 1 
 
 3 
 
 72 
 
 57 
 
 I. 
 
 Indian Territory, protest of Creek delegates against bill extending 
 jurisdiction of Federal courts in 
 
 J. 
 
 Jews in Russia, relative to 
 
 K. 
 
 Keedy, C. M., George W., and Samuel J., executors, report of Court of 
 Claims on case of 
 
 104 
 
 103 
 
 75 
 
 L. 
 
 Library of Congress, report on construction of building for 
 Lilly, Elijah, report of Court of Claims on case of 
 
 M. 
 
 4 
 
 33 
 
 Manson, William T., report of Court of Claims on case of 
 
 Martin, Edmund H., heirs of, report of Court of Claims on case of 
 
 Meaher & Meaher, resolution to refer claim to Court of Claims 
 
 Merrifield, Samuel B., report of Court of Claims on case of 
 
 Mississippi River, levees of the 
 
 Mullendore, Daniel M., report of Court of Claims on case of 
 
 N. 
 
 30 
 
 43 
 
 114 
 
 123 
 
 127 
 
 25 
 
 National Home for Disabled Volunteer Soldiers, report of the Board of 
 
 Managers of the, for 1890 
 
 Neidlinger, Samuel, estate of, report of Court of Claims on case of 
 
 New Mexico, the secretary of, letter from the, in relation to Spanish 
 
 land-grant court J 
 
 New York, resolution relative to fish hatchery in northern 
 
 Nichols, Henry C., report of Court of Claims on case of 
 
 Norton, Sarah E., report of Court of Claims on case of 
 
 Nutt, Julia A., executrix, report of Court of Claims on case of 
 
 38 
 
 44 
 
 96 
 
 46 
 119 
 
 47 
 82 
 
 P. 
 
 Peacock, Martha A., report of Court of Claims on case of.... 
 
 Phelan, Hon. James, eulogies upon 
 
 Phetzing Cornelius, resolution to refer claim of, to Court of Claims 
 
 Pierson, Charles A., et aZ., resolution to reler claims to Court of Claims. 
 
 Ponder, W. M., administrator, report of Court of Claims on case of 
 
 Pope, Henry L., report of Court of Claims on case of 
 
 Public property : 
 
 Report of Clerk of House of Representatives on, in possession of. 
 Report of Doorkeeper, House of Representatives on sale of waste 
 paper 
 
 53 
 
 135 
 
 116 
 
 111 
 
 55 
 
 94 
 
 10 
 
 8 
 
 Vol. 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 8 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 I 
 
VI 
 
 INDEX TO HOUSE MISCELLANEOUS DOCUMENTS. 
 
 Subject. 
 
 No. 
 
 Public Property — Continued. 
 
 Report of Doorkeeper, House of Representatives, submitting inven- 
 tory of 
 
 7 
 
 Q. 
 
 Quinn, Robert, report of Court of Claim on case of. 
 
 R. 
 
 34 
 
 Raiford, Philip, administrator, report of Court'of Claims on case of 
 
 Reformed Church, Sharpsburgh, Md., report of Court of Claims on case 
 
 of 
 
 Rogers, Samuel E., report of Court of Claims on case of 
 
 Roulette, William, report of Court of Claims on case of 
 
 Russell, James B., report of Court of Claims on case of 
 
 Russia, relative to Jews in 
 
 18 
 
 32 
 
 29 
 
 68 
 
 124 
 
 103 
 
 S. 
 
 Saffold, Mary E., report of Court of Claims on case of 
 
 Secretary of War, resolution requesting the, to furnish information 
 
 relative to retired army officers in the civil service 
 
 Sitting Bull, Chief, resolution relative to arrest and killing of 
 
 Skaggs, Ewing M., estate of, report of Court of Claims on case of 
 
 Smith, Grafton F., administrator, report of Court of Claims on case of. 
 
 Smithsonian Institution, report of expenditures of the 
 
 Smithsonian Institution, annual repert for 1890 
 
 South, William B., executor, report of Court of Claims on case of 
 
 Spanish land-grant court, letter from the secretary of New Mexico in 
 
 relation to 
 
 Special messengers, House of Representatives, resolution for appro- 
 priation to pay salary of 
 
 Spencer, C. O., report of Court of Claims on case of 
 
 Stone, Jeff. M., report of Court of Claims on case of 
 
 Stout, Lindsay, representatives of, resolution to refer claim to Court of 
 
 Claims 
 
 Swart, Barnett T., report of Court of Claims on case of 
 
 99 
 
 92 
 
 80 
 
 73 
 52 
 39 
 
 129 
 
 36 
 
 96 
 
 72 
 
 70 
 
 50 
 
 109 
 
 74 
 
 T. 
 
 Tally, J. M. administrator, report of Court of Claims on case of 
 
 Thompson, Abel A., report of Court of Claims on case of 
 
 Tounoir, Lucile, administratrix, report of Court of Claims on case of.. . 
 Treasury Department, report of Second Comptroller in relation to cer- 
 tain claims included in House Ex. Doc. No. 314 Fifty-first Congress, 
 
 first session s 
 
 Turner, John, report of Court of Claims on case of 
 
 Turnley, Parmenus T., report of Court of Claims on case of 
 
 Tweedy, Robert E., report of Court of Claims on case of 
 
 56 
 
 102 
 
 23 
 
 22 
 
 58 
 
 19 
 
 89 
 
 V. 
 
 Van Camp, Aaron, report of Court of Claims on case of 
 
 Von Balsan, R., administrator, report of Court of Claims on case of 
 
 Voters. (See Constitution of the United States.) 
 
 Vulture , Brig, report of Court of Claims on case of 
 
 81 
 
 27 
 
 41 
 
 W. 
 
 Waddell, Charlotte A., executrix, report of Court of Claims on case of. 
 War of the Rebellion, Official Records of: 
 
 Series 1, vol. 31, part 1 - 
 
 Series 1, vol. 31, part 2 
 
 Series 1, vol. 31, part 3 
 
 Series 1, vol. 32, part 1 
 
 69 
 
 12 
 
 13 
 
 14 
 76 
 
 Vol. 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 10,11 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 cn rfi. CO to 
 
INDEX TO HOUSE MISCELLANEOUS DOCUMENTS. 
 
 YII 
 
 Subject. 
 
 No. 
 
 War of the Rebellion, Official Records of — Continued. 
 
 Series 1, vol. 32, part 2 
 
 Series 1, vol. 32, part 3 
 
 Washington and Georgetown Railway Company, annual report of 
 
 Walker, Hon. James, eulogies upon 
 
 Watson, Hon. Lewis, eulogies upon 
 
 Watson Samuel report of Court of Claims on case of 
 
 Western Miama Indians, report of Court of Claims on case of 
 
 Wheeler, William B., executor, report of Court of Claims on case of 
 
 Williams, Mary O., report of Court of Claims on case of 
 
 Woody ard, Mathew, report of Court of Claims on claim of.... 
 
 77 
 
 78 
 91 
 
 134 
 
 133 
 
 15 
 
 83 
 
 49 
 
 20 
 
 88 
 
 Y. 
 
 Young, Thomas P., et ah, resolution to refer claims to Court of Claims.. 112 
 Youngs, Fannie, and Henrietta G., executrics, report of Court of Claims 
 on case of 31 
 
 Z. 
 
 Zoological Park Commission, final report of. 
 
 93 
 
 Vol. 
 
 6 
 
 7 
 
 1 
 
 8 
 8 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
 1 
 
51st Congress, > HOUSE OF REPRESENTATIVES, t Mis. Doc. 
 2d Session. I (No. 136. 
 
 DEPARTMENT OF THE INTERIOR 
 
 BULLETINS 
 
 OF THE 
 
 UNITED STATES 
 
 GEOLOGICAL SURVEY 
 
 NT os. 6*2 t o 65 
 
 WASHINGTON 
 
 GOVERNMENT PRINTING OFFICE 
 
 1891 
 
Title for subject entry. Author title. Series title. 
 
 LIBRARY CATALOGUE SLIPS. 
 
 United States. Department of the interior. ( U. S. geological survey). 
 
 Department of the interior } — ( Bulletin j of the | United 
 States I geological survey | no. 62 | [Seal of the department] | 
 
 Washington | government printing office | 1890 
 
 Second title: United States geological survey | J. W. Powell, 
 director | — | The greenstone schist areas | of the | Menominee 
 and Marquette regions of Michigan | A contribution to the sub- 
 ject of dynamic metamorphism | in eruptive rocks j by [ George 
 Huntington Williams | with an introduction by | Roland Duer 
 Irving | [Vignette] | 
 
 Washington | government printing office | 1890 
 
 8°. 241pp. 16 pi. 
 
 Williams (George Huntington). 
 
 United States geological survey | J. W. Powell, director | — | 
 The greenstone schist areas | of the | Menominee and Marquette 
 regions of Michigan | A contribution to the subject of dynamic 
 metamorphism | in eruptive rocks | by | George Huntington Will- 
 iams | with an introduction by | Roland Duer Irving j [Vignette] | 
 Washington | government printing office | 1890 
 
 8°. 241 pp. 16 pi. 
 
 (United States. Department of the interior. (TJ. S. geological survey). 
 
 Bulletin 62]. 
 
 United States geological survey | J. W. Powell, director | — | 
 The greenstone schist areas | oi the | Menominee and Marquette 
 regions of Michigan | A contribution to the subject of dynamic 
 metamorphism | in eruptive rocks | by | George Huntington Will- 
 iams | with an introduction by | Roland Duer Irving | [Vignette] | 
 Washington | government printing office | 1890 
 6°. 241pp. 16 pi. 
 
 (United States. Department of the interior. ( U. S. geological survey ). 
 Bulletin 62]. 
 
ADVERTISEMENT. 
 
 [Bulletin No. 62.1 
 
 The publications of the United States Geological Survey are issued in accordance with the statute 
 approved March 3, 1879, which declares that— 
 
 “Thepublicationsof theGeological Survey shall consistof the annual report of operations, geological 
 and economic maps illustrating the resources and classification of the lands, and reports upon general 
 and economic geology and paleontology. The annual report of operations of the Geological Survey 
 shall accompany the annual report of the Secretary of the Interior. All special memoirs and reports 
 of said Survey shall be issued in uniform quarto series if deemed necessary by the Director, but other- 
 wise in ordinary octavos. Three thousand copies of each shall be published for scientific exchanges 
 and for sale at the price of publication ; and all literary and cartographic materials received in exchange 
 shall be the property of the United States and form a part of the library of the organization : And the 
 money resulting from the sale of such publications shall be covered into the Treasury of the United 
 States.” 
 
 On July 7, 1882, the following joint resolution, referring to all Government publications, was passed 
 by Congress: 
 
 ‘ ‘ That whenever any document or report shall be ordered printed by Congress, there shall be printed, 
 in addition to the number in each case stated, the ‘ usual number ’ (1,900) of copies for binding and 
 distribution among those entitled to receive them.” 
 
 Except in those cases in which an extra number of any publication has been supplied to the Survey 
 by special resolution of Congress or has been ordered by the Secretary of the Interior, this office has 
 no copies for gratuitous distribution. 
 
 ANNUAL REPORTS. 
 
 I. First Annual Report of the United States Geological Survey, by Clarence King. 880. 8°. 79 pp. 
 1 map.— A preliminary report describing plan of organization and publications. 
 
 II. Second Annual Report of the United States Geological Survey, 1880- '81, by J. W. Powell. 1882. 
 8°. lv, 588 pp. 62 pi. 1 map. 
 
 III. Third Annual Report of the United States Geological Survey, 1881-82, by J. W. Powell. 1883. 
 8°. xviii, 564 pp. 67 pi. and maps. 
 
 IV. Fourth Annual Report of the United States Geological Survey, 1882-83, by J. W. Powell. 1884. 
 8°. xxxii, 473 pp. 85 pi. and maps. 
 
 V. Fifth Annual Report of the United States Geological Survey, 1883-84, by J. W. Powell. 1885. 
 8°. xxxvi, 469 pp. 58 pi. and maps. 
 
 VI. Sixth Annual Report of the United States Geological Survey, 1884-’85, by J. W. Powell. 1885. 
 8°. xxix, 570 pp. 65 pi. and maps. 
 
 VII. Seventh Annual ReportoftheUnitedStatesGeologicalSurvey, 1885-86, by J. W. Powell. 1888. 
 8°. xx, 656 pp. 71 pL and maps. 
 
 VIII. Eighth Annual Report of the United States Geological Survey, 1886— ’87, by J. W. Powell. 1889. 
 8°. 2 v. xix, 474, xii pp. 53 pi. and maps ; 1 p. 1. 475-1063 pp. 54-76 pi. and maps. 
 
 IX. Ninth Annual Report of the United States Geological Survey, 1887-88, by J. W. Powell. 1890. 
 8°. xiii, 717 pp. 88 pi. and maps. 
 
 The Tenth Annual Report is in press. 
 
 MONOGRAPHS. 
 
 I. Lake Bonneville, by Grove Karl Gilbert. 1890. 4°. xx, 438 pp. 51 pi. 1 map. Price $1.50. 
 
 II. Tertiary History of the Grand Canon District, with atlas, by Clarence E. Dutton, Capt. IJ. S. A. 
 1882. 4°. xiv, 264 pp. 42 pi. and atlas of 24 sheets folio. Price $10.12. 
 
 III. Geology of the Comstock Lode and the Washoe District, with atlas, by George F. Becker. 1882. 
 4°. xv, 422 pp. 7 pi. and atlas of 21 sheets folio. Price $11.00. 
 
 IV. Comstock Mining and Miners, by Eliot Lord. 1883. 4°. xiv, 451 pp. 3 pi. Price $1.50. 
 
 V. The Copper-Bearing Rocks of Lake Superior, by Roland Duer Irving. 1883. 4°. xvi, 464 pp. 
 15 1. 29 pi. and maps. Price $1.85. 
 
 VI. Contributions to the Knowledge of the Older Mesozoic Flora of Virginia, by William Morris 
 Fontaine. 1883. 4°. xi, 144 pp. 54 1. 54 pi. Price $1.05. 
 
II 
 
 ADVERTISEMENT. 
 
 VO. Silver-Lead Deposits of Eureka, Nevada, by Joseph Story Curtis. 1884 . 4°. xiii, 200 pp. 16 
 pi. Price $1.20. 
 
 Vin. Paleontology of the Eureka District, by Charles Doolittle Walcott. 1884. 4°. xiii, 298 pp. 
 241. 24 pi. Price $1.10. 
 
 IX. Bracliiopoda and Lamellibranchiata of the Raritan. Clays and Greensand Marls of New Jersey 
 by Robert P. Whitfield. 1885. 4°. xx, 338 pp. 35 pi. 1 map. Price $1.15. 
 
 X. Dinocerata. A Monograph of an Extinct Order of Gigantic Mammals, by Othniel Charles Marsh. 
 1886. 4°. xviii, 243 pp. 561. 56 pi. Price $2.70. 
 
 XI. Geological History of Lake Lahontan, a Quaternary Lake of Northwestern Nevada, by Israel 
 Cook Russell. 1885. 4°. xiv, 288 pp. 46 pi. and maps. Price $1.75. 
 
 XII. Geology and Mining Industry of Leadville, Colorado, with atlas, by Samuel Franklin Emmons. 
 1886. 4°. xxix, 770 pp. 45 pi. and atlas of 35 sheets folio. Price $8.40. 
 
 XIII. Geology of the Quicksilver Deposits of the Pacific Slope, with atlas, by George F. Becker. 
 1888. 4°. xix, 486 pp. 7 pi. and atlas of 14 sheets folio. Price $2.00. 
 
 XIV. Fossil Fishes and Fossil Plants of the Triassic Rocks of New Jersey and the Connecticut Val- 
 ley, by John S. Newberry. 1888. 4°. xiv, 152 pp. 26 pi. Price $1.00. 
 
 XV. The Potomac or Younger Mesozoic Flora, by William Morris Fontaine. 1889. 4°. xiv, 377 
 pp. 186 pi. Text and plates bound separately. Price $2.50. 
 
 XVI. The Paleozoic Fishes of North America, by John Strong Newberry. 1889. 4°. 340 pp. 53 pi. 
 Price $1.00. 
 
 In preparation : 
 
 — Gasteropoda of the New Jersey Cretaceous and Eocene Marls, by R. P. Whitfield. 
 
 — The Penokee Iron-Bearing Series of Northern Wisconsin and Michigan, by Roland D. Irving and 
 C. R. Van Hise. 
 
 — Mollusca and Crustacea of the Miocene Formations of New Jersey, by R. P. Whitfield. 
 
 — Description of New Fossil Plants from the Dakota Group, by Leo Lesquereux. 
 
 — Geology of the Eureka Mining District, Nevada, with atlas, by Arnold Hague. 
 
 — Sauropoda, by O. C. Marsh. 
 
 — Stegosauria, by O. C. Marsh. 
 
 — Brontotheridae, by O. C. Marsh. 
 
 — Report on the Denver Coal Basin, by S. F. Emmons. 
 
 — Report on Silver Cliff and Ten-Mile Mining Districts, Colorado, by S. F. Emmons. 
 
 — Flora of the Dakota Group, by J. S. Newberry. 
 
 — The Glacial Lake Agassiz, by Warren Upham. 
 
 — Geology of the Potomac Formation in Virginia, by W. M. Fontaine. 
 
 BULLETINS. 
 
 1. On Hypersthene- Andesite and on Triclinic Pyroxene in Augitic Rocks, by Whitman Cross, with a 
 Geological Sketch of Buffalo Peaks, Colorado, by S. F. Emmons. 1883. 8°. 42pp. "2 pi. Price 10 cents. 
 
 2. Gold and Silver Conversion Tables, giving the coining values of troy ounces of fine metal, etc., com- 
 puted by Albert Williams, jr. 1883. 8°. 8 pp. Price 5 cents. 
 
 3. On the Fossil Faunas of the Upper Devonian, along the meridian of 76° 30', from Tompkins County 
 N. Y., to Bradford County, Pa., by Henry S. Williams. 1884. 8°. 36 pp. Price 5 cents. 
 
 4. On Mesozoic Fossils, by Charles A. White. 1884. 8°. 36 pp. 9 pi. Price 5 cents. 
 
 5. A Dictionary of Altitudes in the United States, compiled by Henry Gannett. 1884. 8°. 325 pp. 
 Price 20 cents. 
 
 6. Elevations in the Dominion of Canada, by J. W. Spencer. 1884. 8°. 43 pp. Price 5 cents. 
 
 7. Mapoteca Geologica Americana. A Catalogue of Geological Maps of America (North and South), 
 1752-1881, in geographic and chronologic order, by Jules Marcou and John Belknap Marcou. 1884. 
 8°. 184 pp. Price 10 cents. 
 
 8. On Secondary Enlargements of Mineral Fragments in Certain Rocks, by R. D. Irving and C. R. 
 Van Hise. 1884. 8°. 56 pp. 6 pi. Price 10 cents. 
 
 9. AReport of work done in the Washington Laboratory during the fiscal year 1883-84. F. W. Clarke, 
 chief chemist. T. M. Chatard, assistant chemist. 1884. 8°. 40 pp. Price 5 cents. 
 
 10. On the Cambrian Faunas of North America. Preliminary studies, by Charles Doolittle Walcott. 
 1884. 8°. 74 pp. 10 pi. Price 5 cents. 
 
 11. On the Quaternary and Recent Mollusca of the Great Basin ; with Descriptions of New Forms, by 
 R. Ellsworth Call. Introduced by a sketch of the Quaternary Lakes of the Great Basin, by G. K. 
 Gilbert. 1884. -8°. 66 pp. 6 pi. Price 5 cents. 
 
 12. A Crystallographic Study of the Thinolite of Lake Lahontan, by Edward S. Dana. 1884. 8°. 
 34 pp. 3 pi. Price 5 cents. 
 
 13. Boundaries of the United States and of the several States and Territories, with a Historical 
 Sketch of the Territorial Changes, by Henry Gannett. 1885. 8°. 135 pp. Price 10 cents. 
 
 14. The Electrical and Magnetic Properties of the Iron-Carburets. by Carl Barus and Vincent 
 Strouhal. 1885. 8°. 238 pp. Price 15 cents. 
 
 15. On the Mesozoic and Cenozoic Paleontology of California, by Charles A. White. 1885. 8°. 
 33 pp. Price 5 cents. 
 
ADVERTISEMENT. 
 
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DEPARTMENT OP THE INTERIOR 
 
 BULLETIN 
 
 OF THE 
 
 UNITED STATES 
 
 GEOLOGICAL SURVEY 
 
 No. 62 
 
 WASHINGTON 
 
 GOVERNMENT PRINTING OFFICE 
 1890 
 
UNITED STATES GEOLOGICAL SURVEY 
 
 J. W. POWELL, DIRECTOR 
 
 THE GREENSTONE SCHIST AREAS 
 
 OF THE 
 
 A CONTRIBUTION TO THE SUBJECT OF DYNAMIC METAMORPHISM 
 IN ERUPTIVE ROCKS 
 
 BY 
 
 GEORGE HUNTINGTON WILLIAMS 
 
 WITH AN INTRODUCTION BY 
 
 ROLAND DUER IRVING 
 
 WASHINGTON 
 
 GOVERNMENT PRINTING OFFICE 
 1890 
 
CONTENTS. 
 
 Page. 
 
 Letter of transmittal, by R. D. Irving 9 
 
 Explanatory and historical note, by R. D. Irving 11 
 
 Introduction 31 
 
 Chapter I. Present state of our knowledge regarding the metamorphism of 
 
 eruptive rocks 34 
 
 Value of the microscope in the study of metamorphism 34 
 
 Historical outline of studies on the metamorphism of eruptive rocks 40 
 
 Chapter II. Greenstone belts of the Menominee iron district 64 
 
 Introductory and historical 64 
 
 Sturgeon Falls 67 
 
 Lower, or Little Quinnesec Falls 77 
 
 Chapter III. Greenstone belts of the Menominee iron district (continued). .. 96 
 
 Upper, or Big Quinnesec Falls 96 
 
 The dark colored greenstones of the basin 97 
 
 The light colored greenstones at Upper Quinnesec falls 102 
 
 The coarse grained diorites of the Horse Race 106 
 
 The acid rocks of the Upper Quinnesec Falls and Horse Race 110 
 
 Four- foot Falls 123 
 
 The Twin Falls 127 
 
 Lower Twin Falls 129 
 
 Upper Twin Falls. 132 
 
 Chapter IV. Greenstone belts of the Marquette district 134 
 
 Introductory 134 
 
 Rocks of the northern portion of the Marquette area 138 
 
 Basic intrusives 138 
 
 Acidintrusives 146 
 
 Banded greenstone schists 154 
 
 Chapter V. Greenstone belts of the Marquette district (continued) 163 
 
 Rocks of the southern portion of the Marquette area 163 
 
 The aphanitic greenstones 163 
 
 Coarse grained dike rocks 168 
 
 Greenstones south of the quartzite 170 
 
 Rocks of the Negauuee area 171 
 
 Aphanitic greenstones 171 
 
 Coarsely crystalline greenstones 173 
 
 The stretched fragmental rocks on the Carp River 175 
 
 Acid rocks 178 
 
 Rocks of the Northern area. 179 
 
 Unaltered basic intrusives 180 
 
 Altered coarse grained rocks 180 
 
 Banded greenstones 184 
 
 Green schists and agglomerates of Deer Lake 185 
 
 5 
 
6 
 
 CONTENTS. 
 
 Page. 
 
 Chapter VI. — General results and conclusions 192 
 
 Original character of the Menominee and Marquette greenstone areas 192 
 
 Evidence of eruptive character 192 
 
 Different original rock types 197 
 
 Original mineral constituents 199 
 
 Conditions under which the greenstones were formed 200 
 
 Macrostructural metamorphism of the Menominee and Marquette massive 
 
 rocks 201 
 
 Macrostructural metamorphism through compression, faulting, or 
 
 crushing 202 
 
 Macrostructural metamorphism through stretching 204 
 
 Microstructural metamorphism of the Menominee and Marquette massive 
 
 rocks 204 
 
 Effects of dynamic action on individual minerals 205 
 
 New structures produced by dynamic action 206 
 
 Mineralogical (chemical) metamorphism of the Menominee and Marquette 
 
 massive rocks 208 
 
 Secondary minerals and their origin 209 
 
 Progress of alteration in the original minerals 214 
 
ILLUSTRATIONS. 
 
 Plate I. Outline geological map of the Marquette region 
 
 II. Outline geological map of the Menominee iron region 
 
 III. Map of Sturgeon Falls, Menominee River (after Brooks) 
 
 IV. Map of Lower Quinnesec Falls, Menominee River (after Brooks). 
 
 V. Map of Upper Quinnesec Falls, Menominee River (after Brooks) . 
 
 VI. Map of Twin and Four-toot Falls, Menominee River (after Brooks) 
 
 VII. Map of the environs of Marquette 
 
 IX. 
 
 XVI. 
 
 Fig. 
 
 1 . 
 
 
 2. 
 
 Fig. 
 
 1 . 
 
 
 2. 
 
 Fig. 
 
 1 . 
 
 
 2. 
 
 Fig. 
 
 1 . 
 
 
 2. 
 
 Fig. 
 
 1 . 
 
 
 2. 
 
 Fig. 
 
 1 . 
 
 
 2. 
 
 Fig. 
 
 1 . 
 
 
 2. 
 
 Fig. 
 
 1 . 
 
 
 2. 
 
 Fig. 
 
 1 . 
 
 Saussurite gahbro (first stage) 
 
 2. Saussurite gabbro (second stage) 
 
 1. Altered diabase or diorite 
 
 2. Schistose band in the last figured rock, showing the effect 
 
 of dynamic metamorphism (stretching) upon it 
 
 1. Saussurite diorite 
 
 2. Typical aphanitic greenstone of the Marquette region.. 
 
 1. Chlorite-epidote aggregate in an altered diabase 
 
 2. Stretched greenstone 
 
 1. Coarsely crystalline diorite 
 
 2. Epidiorite 
 
 1. Sphene crystals around ilmenite 
 
 Rutile originating from the alteration of ilmenite 
 
 1. Sericite porphyry 
 
 Stretched and brecciated greenstone 
 
 1. Structure of one of the u eyes” in an “Augengneiss ” or 
 
 stretched granite porphyry 
 
 2. Stretched quartz porphyry 
 
 1. Greenstone schists (tuffs) of the northern Marquette area 
 
 Ampliibole granite (?) forming a dike in the aphanitic 
 greenstones 
 
 Page. 
 
 14 
 
 24 
 
 68 
 
 86 
 
 96 
 
 124 
 
 138 
 
 222 
 
 222 
 
 224 
 
 224 
 
 226 
 
 226 
 
 228 
 
 228 
 
 230 
 
 230 
 
 232 
 
 232 
 
 234 
 
 234 
 
 236 
 
 236 
 
 238 
 
 238 
 
 Fig. 1. Hypothetical section of the Menominee region in the vicinity of 
 
 Quinnesec (after Brooks) 26 
 
 2. Hypothetical section of the Menominee region in the vicinity of Twin 
 
 Falls (after Brooks) 27 
 
 3. Hypothetical section of the Menominee region in the vicinity of Quin- 
 
 nesec (by R. D. Irving) 30 
 
 4. Twinning lamellie in secondary albite 69 
 
 5. Zoisite crystals in saussurite 69 
 
 6. Zoisite crystal showing position of optical constants with reference to 
 
 cleavage lines 70 
 
 7. Compact and fibrous secondary hornblende 70 
 
 8. Helminth (vermicular chlorite) in quartz 71 
 
 9. Hornblende altering to chlorite 79 
 
 10. Cross gashes in greenstone produced by stretching 81 
 
 11 . Broken feldspar crystals in crushed and stretched greenstone 105 
 
 7 
 
8 
 
 ILLUSTRATIONS. 
 
 Page. 
 
 Fig. 12. Rutile needles (Thonschiefernadeln) 106 
 
 13. Broken tourmaline crystal proving the secondary fracture of the in- 
 
 closing quartz 112 
 
 14. Foliated granite (gneiss) intrusive in greenstone 115 
 
 15. Foliated granite (gneiss) intrusive in greenstone 115 
 
 16. Foliated granite (gneiss) intrusive in greenstone 116 
 
 17. Orthite (allanite) in granite 117 
 
 18. Broken zircon crystal in schistose porphyry 122 
 
 19. Compact surrounded by fibrous hornblende (secondary growth?) 126 
 
 20. Rhomboidal parting in greenstone (diagrammatic) 128 
 
 21. Acute rhomboidal parting in greenstone (diagrammatic) 128 
 
 22. Schistose parting developed from that in Fig. 21 128 
 
 23. Greenstone made schistose by faulting 129 
 
 24. Greenstone made schistose by faulting 130 
 
 25. Anatase formed by the alteration of ilmenite in greenstone 131 
 
 26. Spheroidal parting of aphanitic greenstone produced by brecciation.. 166 
 
 27. Same as in Fig. 26, drawn out into lenses by pressure 177 
 
 28. Bent hornblende crystal 183 
 
 29. Surface of agglomerate from Deer Lake 188 
 
LETTER OF TRANSMITTAL. 
 
 United States Geological Survey, 
 
 Lake Superior Division, 
 Madison , Wisconsin , February 10, 1888. 
 
 Sir : I have the honor to transmit herewith, for publication as a 
 bulletin of the Survey, a paper, by Prof. George H. Williams, of Balti- 
 more, Maryland, on The Greenstone-Schist Areas of the Marquette and 
 Menominee Regions of Michigan. 
 
 The exact object and bearing of the work thus accomplished by 
 Prof. Williams I have set forth in an explanatory and historical note 
 prefixed to his memoir. 
 
 I am, sir, very respectfully, yours, 
 
 R. D. Irving, 
 
 Geologist in Charge . 
 
 Hon. J. W. Powell, 
 
 Director U. S. Geological Survey. 
 
 9 
 
EXPLANATORY AND HISTORICAL NOTE. 
 
 By Roland Duer Irvino. 
 
 At quite a number of points in the Lake Superior region occu* pecu- 
 liar schistose rocks, which combine with a prevalent fi ne grain a general 
 tendency to greenish color. Besides occurring here and there more or 
 less confusedly mingled with masses of granite and other rocks, these 
 greenish schists occur also in large continuous areas, which they entirely 
 occupy, except for certain relatively unimportant basic and acid intru- 
 sives. Microscopic study has shown that these rocks are at times fully 
 developed hornblende schists, and again glossy kinds, in which chlorite 
 is so important an ingredient as to warrant our calling them chlorite 
 schists. In other places again they are more massive, and present more 
 or less distinctly the appearance of fine-grained basic eruptives; but 
 the bulk of these areas is composed of nondescript fine-grained green- 
 ish schists, which appear to grade into the more massive greenstone-like 
 forms on the one hand, and into the more distinctly developed chloritic 
 and hornblendic schists on the other. As a rule these various schists 
 present no parallel structure other than that which seems referable 
 directly to secondary causes ; that is to say, they do not present such 
 banded varieties as would suggest the action of sedimentation during 
 their production. However, such banded varieties do occur in subordi- 
 nate quantity, presenting then very strikingly regular, rapid alterna- 
 tions of light and dark bands. 
 
 Again, here and there in these peculiar areas, in some places with a 
 very considerable development, there occur kinds which present a more 
 or less obscure fragmental appearance, this appearance being generally 
 far more pronounced on a weathered surface than on a fresh one, on 
 which latter the matrix and the parent fragments are apt to look much 
 like one another, either from original similarity in character or from 
 having undergone alterations which have led both fragments and 
 matrix, originally different, to similar results. At times there is a co- 
 incidence of occurrence between the banding above referred to and the 
 appearance of the pebble-bearing forms, but so far as my experience 
 goes this is very commonly not the case, the fragmental phases being 
 without any parallel structure other than the general secondary cleav- 
 age, which all of these rocks present, the apparent pebbles occurring 
 more commonly in tumultuous assemblages of masses of all sizes. 
 
12 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 As prominent illustrations of such green schist areas, there may be 
 mentioned that which runs directly westward from the shore of Lake 
 Superior at Marquette, Michigan, for a distance ofj some twenty miles, 
 with a width ranging from two to six miles ; 1 those which occur in the 
 Menominee Yalley, on the boundary between Wisconsin and Michigan; 2 
 that of the Gogebic country of western Michigan, in T. 47 NT., E. 43 W., 
 and T. 47 N., E. 44 W., where there is a very great development of the 
 fragmental phases; 3 that which has been recently outlined by Dr. W. 
 
 S. Bayley to the south of the so-called Mesabe Eange, and west of 
 the Embarras Lakes, in T. 59 N., E. 15 W., and T. 59 N., E. 16 W., 
 northern Minnesota, where there is again a considerable development 
 of the fragmental forms ; 4 and that which lies to the northward of the 
 iron-bearing slates of Yermillion Lake, traversing the island in the 
 northern part of that Jake from west to east, and extending thence east 
 and northeast, with an average width of from two to three miles, through 
 townships 62, 63, 64, and 65 N., of ranges 14, 13, 12, 11, 10, and 9 W., in 
 northern Minnesota, to the national boundary line at Carp Lake, whence 
 it extends an unknown distance into Canada. This last-named area, 
 which is the most extended continuous one with which I am acquainted, 
 shows prevalently those kinds of rock which lack the fragmental ap- 
 pearance. Still, fragmental phases here and there present themselves, 
 as, for instance, along the east shore of that island in Yermillion Lake, 
 which lies in the northern part of Sec. 10 and southern part of Sec. 3, 
 
 T. 62 N., E. 16 W. To these areas may be added also several smaller 
 ones which lie southward and southeastward of the Yermillion Lake iron 
 belt. One of these areas, lying south of Sea Gull Lake and east of 
 Ogishkimanissi Lake, in T. 65 N., E. 5 W., presents an extraordinary 
 development of the obscurely fragmental or brecciated phase. Finally, 
 should be mentioned the large development of similar greenish schists, 
 including also the fragmental or “ agglomeratic ” phases, which is 
 described as occurring on the Lake of the Woods in the recent report 
 of Mr. A. C. Lawson, of the Canadian Survey. 5 
 
 My first acquaintance with any of these green schist areas was in the 
 summer of 1883, when a number of days were spent in examining the 
 exposures at Twin Falls, Upper Quinnesec Falls and Lower Quinnesec 
 Falls, on the Menominee Eiver, the boundary between Wisconsin and 
 Michigan. The very handsome detailed maps and the descriptions of 
 these exposures by Maj. T. B. Brooks 6 had already been published and 
 
 1 See map of T. B. Brooks, Geol. Survey Michigan, Atlas, PI. Ill $ map by C. Kominger, accompany- 
 ing Geol. Survey Michigan, Vol. 4, 1881 ; PI. I of the present volume. 
 
 2 See map by T. B. Brooks and C. E. Wright, PI. 28 of the atlas to the Geology of Wisconsin ; map 
 by C. E. Wright, PI. 30 of the same atlas ; map of the Menominee region, by C. Rominger, Geol. Sur- 
 vey Michigan, Vol. 4, 1881, PI. 2. 
 
 3 See maps by It. D. Irving and C. It. Van Hise, accompanying a memoir on the Penokee-Gogebio 
 iron region, Mon. U. S. Geol. Survey, No. 18. 
 
 4 See map by It. D. Irving, PI. XLI, of the Seventh Ann. Kept. U. S. Geol. Survey. 
 
 6 See Geol. Nat. Hist. Survey Canada, Ann. Rep. (new series) Vol. 1, 1885, pp. 41-46 cc; also map 
 accompanying same. 
 
 6 Ge[>l. Wisconsin, vol. 3, 1880. 
 
iBvufG. 1 EARLY IMPRESSIONS OF MENOMINEE GREENSTONES. id 
 
 were used on the ground. These maps represent the exposures at the 
 several points named as composed of a series of very regular alterna- 
 tions of various schistose and massive rocks, the conclusion being 
 reached with regard to them by Brooks that they form in all a regular 
 series of layers originally of sedimentary origin, the present lack of frag- 
 mental appearance being taken as the result of metamorphism. To me 
 it seemed at that time that the regularity of the alternations was far 
 less than one would think to be the case from Brooks’s maps, and that all 
 of the several phases, schistose and non- schistose, were rather vari- 
 ations of one great mass of material, whose original structure was mass- 
 ive rather than schistose. This impression was gathered from the way 
 in which the several phases graded into one another, and from the non- 
 continuity in the direction of the strike of the schistose kinds, single 
 schist beds displayed on one side of the stream being often absent 
 where their continuations should lie on the opposite side of the stream. 
 The impression was strengthened by the lack of regularity in the di- 
 rection of the schist planes, and by the striking way in which schist 
 bands inclose vaguely outlined areas of non-schistose massive rocks. 
 The same conclusion as to the inseparable nature of all of these rocks 
 had already been reached and published by Rominger, 1 though he ap- 
 pears to have looked upon the parallel or schistose structure as repre- 
 senting an original condition of the rocks, all of which he seems to 
 consider of sedimentary origin; while the impression made on me was 
 iust the opposite, namely, that the schistosity is of a secondary nature, 
 and the original structure of the rock a massive one. In order to test 
 this question, a large collection of specimens, with quite full notes, was 
 made at the time. In the next year, however, before the thin sections 
 made from these specimens could be examined, the entire collection 
 was destroyed by fire, and my work in other directions having 
 become pressing, it was decided to put the study of this question in 
 the hands of Prof. George H. Williams, of the John Hopkins Uni- 
 versity, whose qualifications for investigations in microscopic petrog- 
 graphy, such as this would mainly be, are well known to be of the first 
 order. In the summer of 1885, therefore, Professor Williams made, at 
 my request, a reexamination of all of these points in the Menominee 
 valley, going into far greater detail in the field study than any one 
 had done before, and collecting on a very large scale. During the 
 summer of 1886, Professor Williams was asked to extend his field ex- 
 aminations into the Marquette greenschist area, and here similar de- 
 tailed studies and large collections were made. The present publica- 
 tion is the result of Professor Williams’s work, which has included the 
 detailed examination of about 400 thin sections made from the speci- 
 mens gathered. 
 
 While Professor Williams’s investigations have been going on, the 
 various other green schist areas named, so far as they lie within the 
 
 Geol. Survey Michigan, vol. 4 , 1881, p. 214. 
 
14 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 . 
 
 boundary of the United States, have been examined in considerable de- 
 tail, large collections and extensive field-notes having been gathered by 
 Prof. Yan Hise, Messrs. W. N. Merriam and W. S. Bay ley, and myself. 
 These additional collections are now quite thoroughly sectioned, and it 
 is hoped soon to study them in detail, and to offer a second contribution 
 to our knowledge of this important class of rocks. The present publi- 
 cation, however, deals only with the Marquette and Menominee areas. 
 
 Prof. Williams’s investigations having been directed especially to a 
 microscopic study of these peculiar greens chists, with the object of ascer- 
 taining whether such study would throw any light upon their original 
 condition ; it does not come within the province of his memoir to discuss 
 the geologic relations of the green schist masses as wholes. Neverthe- 
 less, it is almost unavoidable that some reference should be made in this 
 volume to these geological relations, and, since there has been a good 
 deal of difference of opinion as to them among the several geologists 
 who have written upon the Menominee and Marquette areas, it seems 
 necessary to explain briefly the different views that have been advanced, 
 including the conclusions to which my own studies have thus far led me, 
 though without attempting any general discussion of the subject for 
 the whole Lake Superior region. Such a discussion it is designed to leave 
 until exhaustive microscopic studies, like that of Professor Williams here 
 presented, shall have been extended over the other areas of similar rocks 
 above named. We shall then be in possession not only of all available 
 structural facts with regard to these peculiar rocks, but also of all that 
 the most refined methods of study can give us with regard to their in- 
 ternal texture and mineralogical composition. 
 
 The map (PI. I) shows, in a general way, the distribution of the dif- 
 ferent kinds of rocks in the vicinity of Marquette. In preparing this 
 map, those by Brooks and Bominger, read in the light of my own studies 
 in this region, have been used. It should be said that a detailed map 
 of the Marquette district has not been attempted by the U. S. Geologi- 
 cal Survey as yet, partly because other more pressing work was in prog- 
 ress, and partly because without a thoroughly accurate topographical 
 basis for such a map it has not been thought that much advance could 
 be made upon the several maps heretofore constructed. It is proposed, 
 however, to begin such topographical survey immediately, and upon 
 the basis thus prepared, to place everything exactly as it is seen, and, 
 making use of all the latest mining developments, to attempt to work 
 out accurately and in detail the structure of the region in such a fash- 
 ion that what is inferred may be easily separated from what is actually 
 known. 
 
 Upon the present map the large area colored for greenstone schists 
 is the one which came particularly under Professor Williams’s investiga- 
 tions. Northward this area is limited, in the eastern portion, by a great 
 spread of granitic and gneissic rocks. The line of demarkation between 
 the schists and the granites, however, is not a sharp one, since the 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILUNOIS 
 
U.S. GEOLOGICAL SURVEY. 
 
 R.27 W. 
 
 ARCH EAN. 
 
 AGE L 
 
 Granite and Gneiss. Greenstone Schists. Altered 
 
 wm 
 
 OUTLINE GEOLOGICAL MAI 
 
 Compiled by R.D.Irviiuj ir omnia 
 
 Scab 
 
BULLETIN No. 62 PLATE I. 
 
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 v/ / w C*Si*£ 
 
 
 
 >T*'i v 
 
 Cccrp A* t 
 
 M£-s\ 
 
 ' Goose ItcLke 
 
 ,NOWN. 
 
 ALGONKI AN. 
 
 CAMBRIAN. 
 
 'itlolitt 
 
 Iron Bearing Serie s . Lake Superior S. S . 
 < Detritals, Limestones and 
 Femujinous Schists, with interbedded 
 Greenstones.) 
 
 I~aT~| 
 
 €s 
 
 DF THE MARQUETTE REGION. 
 
 by T.B.Rrooks and (’.Romincjer. 
 miles. 
 
 ,9 
 
til 
 
IBV1NG.1 
 
 GREENSTONE SCHISTS NEAR MARQUETTE. 
 
 15 
 
 two seem to mingle more "or less confusedly on each side of the some- 
 what arbitrary line indicated upon the map. Southward of this green- 
 stone-schist area, and again dovetailing into it on the north, are belts 
 of country occupied mainly by detrital rocks, such as quartzites and 
 various fragmental slates; with these, however, are large bodies of 
 crystalline limestone and several phases of ferruginous schist, all 
 of which have in common an entire lack of anything like a frag- 
 mental texture. In addition to these rocks these areas include also 
 sheets of diabasic greenstone, which are interbedded with the detritals 
 and ferruginous schists alluded to. On the south of the southernmost 
 of these detrital areas, in which are included all the well known iron 
 mines of the Marquette region, is again a large area of granitic and 
 gneissic rocks. 
 
 The greenstone schists are affected generally by a vertical or nearly 
 vertical cleavage structure, to which the occasional banding of the 
 rock, suggestive of a sedimentary origin, is also parallel. The layers 
 of rock of which the detrital areas are composed are affected partly by 
 a similar cleavage structure, but, on the whole, far less markedly so, 
 while the bedding of these rocks is as a rule very distinct, and indi- 
 cates a more or less open or gentle bowing of the layers, the dips being 
 at times southward and again northward, and usually at a much lower 
 angle than is the cleavage structure of the greenstone schists. At 
 times, however, particularly in the easternmost portion of the southern 
 of these two belts, the inclinations of the detrital rocks are much higher, 
 and then bedding and cleavage structure approach to parallelism with 
 each other, and with the cleavage structure of the greenstone schists 
 further north. While folded back and forth, these detrital areas show 
 for the most part an evident general synclinal structure; that is to say, 
 the layers of rock of which they are composed, as they appear along the 
 edges of these areas, dip inward towards their middle portions. Thus 
 the greenstone schists seem plainly to rise from beneath the higher de- 
 trital layers. As to the inferior position of these greenstone schists to 
 the detrital iron-bearing rocks, all geologists who have examined this 
 region would probably agree; at all events all those who have expressed 
 themselves with regard to the matter seem to have no hesitation con- 
 cerning it. 
 
 Foster and Whitney, whose classical work 1 gives the first compre- 
 hensive account of the geology of this region, do not appear to have 
 separated the greenstone schists from the other stratiform rocks in such 
 a fashion as to indicate their exact strati graphical relations. All of 
 these stratiform rocks they appear to have looked upon as constituting 
 one great series, whose crumpled condition they attributed to the sub- 
 sequent eruption of the granite masses on either side of the single 
 trough, which they regarded the stratiform rocks as occupying . 2 They 
 
 •Report of the geology of the Lake Superior land district, by J. W. Foster and J. D. Whitney, pt. 2. 
 The Iron Region, Washington, 1851. 
 
 ’Ibid., p. 41, Fig. 5. 
 
16 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 appear, however, to refer especially to the greenstone schists in the 
 following: 
 
 Many of the slates appear to be composed of pulverulent greenstone, as though they 
 might originally have been ejected as an ash, and subsequently deposited as a sedi- 
 ment, and pass by imperceptible gradations, from a highly fissile to a highly compact 
 state. * * * The slates are composed essentially of the same ingredients as the 
 trappean rocks with which they are associated, and the main difference between 
 them may be that the one was the product of salses, ejected in the form of mud, while 
 the other was the product of volcanoes, ejected in molten streams . 1 
 
 They appear also to refer especially to the greenstone schists when 
 they speak of the stratiform series as exhibiting greater alteration in 
 the vicinity of the masses of eruptive granite, than at distances from 
 these masses. 2 
 
 J. P. Kimball, who wrote in 1864, 3 considered the granitic and gneissic 
 masses on either side of the belt of stratiform rocks, as correspond- 
 ing to the Laurentian series of Canada, while he parallelized the whole 
 of the stratiform succession with the Huronian series of the north shore 
 of Lake Huron, thus making the granitic and gneissic rocks the older 
 basement upon which all of the stratiform Huronian was subsequently 
 spread, wholly by aqueous agencies. None of the various rocks which 
 Foster and Whitney looked upon as eruptive, are thought by Kimball 
 to have had that origin, even the various greenstones being taken to be 
 metamorphic sedimentary material. In the case below Kimball appears 
 to refer particularly to the greenstone schists, which form our present 
 subject, and which, it thus appears, he looked upon as the basement 
 member of the Huronian succession. He says: 4 
 
 The gneiss which marks the boundary of the granite belts, and accordingly char- 
 acterizes the top of the Laurentian series in this region, the same as it is elsewhere 
 represented, is succeeded by dark colored hornblendic schists, which consequently 
 represent the base of the Azoic or Huronian series. These schists are followed by a 
 series of augitic rocks and schists, interstratified with magnesian hydrous rocks and 
 slates, the two kinds of rocks being represented on the one hand by hypersthene, pyr- 
 oxene, and bedded diorite passing into dioritic slates, and on the other by talcose 
 and chloritic schists. The former character of rocks prevails to such an extent as to 
 impart to the lower members of the Huronian series a distinctive augitic aspect. 
 The several rocks composing this augitic zone are commonly of a greenish color, and 
 vary in this respect chiefly as to shade, resembling in this particular the Lower Slate 
 Conglomerate, which marks the base of the series in Canada, and from which they 
 seem to differ only in the absence of pebbles and bowlders from the subjacent Lau- 
 rentian rocks, which there form a distinguishing feature . 5 * 
 
 1 Report of the geology of the Lake Superior land district, by J. W. Foster and J. D. Whitney, pt. 2. 
 The Iron Region, Washington, 1851, pp. 16, 17. 
 
 2 Ibid., p. 14. 
 
 3 Am. Jour. Sci., 2d series, vol. 39, 1865, pp. 290-303. 
 
 4 Ibid., p. 294. 
 
 6 This supposed similarity of the greenstone schists of Marquette to the Lower Slate Conglomerate 
 of Lake Huron is not borne out at all by later microscopic and field studies. Indeed, the two have 
 nothing whatever in common, unless the occasional greenish color of the Lake Huron rocks be taken to 
 indicate such a resemblance. The Lower Slate Conglomerate of Lake Huron, with its granitic and 
 gneissic pebbles, proves to be a mostcompletely detrital and plainly water- formed mass composed chiefly 
 of fragments of quartz and feldspar, with the alteration products of the latter, the whole cemented by 
 a silicious paste. This statement is made only after a careful examination of the Labe Huron region, 
 and after the study of a ver}- large number of thiu sections from Logan's so-called Lower Slate Con- 
 glomerate. 
 
IRVING.] 
 
 MARQUETTE GREENSTONES. 
 
 17 
 
 T. B. Brooks, upon his detailed map of the Marquette district 1 leaves 
 blank the larger part of the area occupied by the greenstone schists 
 which now especially concern us, indicating here and there upon it, 
 however, the occurrence of belts of “diorite” and of “chloritic and 
 dioritic schists. 1 ’ All of these rocks he evidently regards as belonging 
 conformably beneath the detrital quartzites and slates which form his 
 division No. V, of the iron-bearing series, which division appears in a 
 bold ridge along the northern edge of the southern of the two detrital 
 areas indicated on the outline map herewith. The diorites Brooks 
 classes lithologically with the greenstones interstratified with the de- 
 trital rocks themselves, though apparently looking upon them as be- 
 longing to much lower layers in the succession. In this lithological 
 correlation, as will be seen in the sequel, Brooks was largely correct, 
 since the diorites of the greenstone schist area prove to be diabasic 
 greenstones in dike form, and to be entirely similar lithologically to the 
 interbedded greenstones of the detrital or iron-bearing areas, with which 
 they are also presumably wholly ‘contemporaneous. All of these rocks, 
 both massive and schistose, Brooks plainly regarded as metamorphosed 
 water-formed sediments. 
 
 Wadsworth, writing in 1880, 2 advocates in the main the views 
 presented by Foster and Whitney, as will be seen by the following 
 quotation : 
 
 The general structure of the country would seem to be as follows : The schists, 
 sandstones, etc., having been laid down in the usual way, were then disturbed by the 
 eruption of the jasper and ore ; this formed the knobs of jasper, the bauding belong- 
 ing to the fluidal structure, and not to sedimentation. Besides occurring in bosses, 
 the jasper was spread out in sheets, and intruded through the rock in wedge-shaped 
 masses, sheets, and dikes. Much of the original rock still remained horizontal, and 
 new sedimentary deposits continued to be formed out of the jasper and the other rocks. 
 Next came the eruption of “ diorite,” which completed most of the local folding and 
 tilting of the strata. Finally, the granite eruption took place on both sides of the 
 “ Huronian,” uplifting and contorting the strata near it, and perhaps laterally com- 
 pressing the inclosed iron-bearing rocks . 3 
 
 Dr. Wadsworth does not appear to express any particular opinion as 
 to the strati graphical position of the greenstone schists of the area now 
 especially under consideration, speaking of them only in connection 
 with all the rest of the stratiform rocks of the region as older than the 
 adjacent granite areas. The greater part of these greenstone schists 
 he would seem to have looked upon as certainly sedimentary, 4 since he 
 records a number of observations going to show that there is no grada- 
 tion between them and certain dike-like masses occurring with them, 
 using these observations in opposition to the ideas expressed by some 
 of his predecessors to the effect that inasmuch as the massive rocks and 
 
 'Geol. Survey, Michigan, 1873, vol. 1, Atlas pi. 3. See also pp. 99-104, same vol. 
 
 3 Notes on the Geology of tho Iron and Copper Districts of Lake Superior. By M. E. Wadsworth 
 Bull. Mus. Comp. Zool. Harvard College, Wholo Scries, vol. 7 (Geol. Series, vol. 1 No. 1). 
 
 9 Ibid., p. 75. 4 Ibid., p. 37. 
 
 Bull. 62 § 
 
18 GREENSTONE SCHIST AREAS OF MICHIGAN. Ibull. 62 . 
 
 the schists grade into one another, the former are of sedimentary origin 
 as well as the latter. That there are genuine dikes intersecting these 
 schists and having no gradations into them, Professor Williams’s observa- 
 tions recorded in this volume, as well as those by Rominger and others, 
 make very plain, although even in the case of these genuine later dikes 
 there are at times partially schistose forms produced apparently by 
 secondary dynamic agencies. On the other hand, it will be seen from Pro- 
 fessor Williams’s descriptions that there are other massive forms among 
 these greenstone schists which do present every possible gradation into 
 the schists themselves, and must, therefore, be believed to have had a 
 common origin with them. 
 
 Rominger, in his account of the geology of the Marquette region, 
 published in 1881, 1 describes very fully the greenstone-schist area which 
 Professor Williams has studied. Rominger’s mapping of this area has 
 essentially been followed upon the small sketch-map accompanying the 
 present volume. The rocks of this area lie describes under the gen- 
 eral head of the u dioritic group,” which group he looks upon as form- 
 ing the basement member of the Huronian series within which he would 
 include all the stratiform rocks of the region, considering it as placed 
 conformably beneath the detrital strata. The origin of the structure 
 of these greenstone schists he looks upon as having been a secondary 
 one, although he recognizes distinctly their intrusion by later genuinely 
 eruptive dikes. Inasmuch as in its more northern portion the green- 
 stone-schist area presents numerous bosses and veins of gTanite, he 
 considers these as proving the more recent origin of the great granite 
 masses lying both to the north and south of all stratiform rocks, thus 
 returning, as did Wadsworth before him, to the early expressed view 
 of Foster and Whitney, with whom he agrees also in considering that 
 the crumpling of all of the stratiform rocks, greenstone schists and de- 
 tritals as well, has been accomplished by the protrusion of the later 
 granite masses on either side. In the same volume, and upon his map, 
 Dr. Rominger indicates numerous small areas of massive and schistose 
 greenstones as occurring in the vicinity of Negaunee and Ishpeming, 
 within the district represented on the outline map herewith, as occupied 
 entirely by the detrital iron-bearing series. These masses he regards 
 as forming portions of his dioritic group, although at the same time 
 recognizing distinctly the fact that they occur at various horizons 
 among the detritals, which he looks upon as lying wholly above the 
 main mass of his dioritic rocks. This anomalous arrangement he ex- 
 plains by representing that the dioritic group, inasmuch as it lies at 
 the base of the entire stratiform series, comes directly into contact 
 with the granite protrusions, whose metamorphosing influence was so 
 great as to cause the fusion of a portion of these basement layers. 
 These fused portions, then, he imagines to have intruded themselves 
 in various shapes among the higher detrital layers. 2 This view, how- 
 
 1 Geol. Survey Michigan, 1881, vol. 4, with map of Marquette region, 
 
 2 Ibid., pp. 22-39, particularly pp. 37, 38. 
 
IRVING.] 
 
 MARQUETTE GREENSTONES. 
 
 19 
 
 ever, Dr. Rominger subsequently abandoned, as will appear from the 
 following quotation from the manuscript of his last and yet unpub- 
 lished report : l 
 
 As from the massive form of the diorites a gradation exists into the schistose con- 
 dition, and as schistose structure formerly appeared to me a positive proof of a 
 former sedimentary origin, I resorted in my previous report, in order to explain the 
 similarity in the composition ofithe schists with the massive diorites, to the hypoth- 
 esis of a secondary fusion of the lower beds of sediments nearest to the focus of cen- 
 tral heat, and subsequent injection of the fused part into the folds and fissures of 
 the remainder of the strata, simultaneously also the molten mass to have been forced 
 into the fissures and crevices of the adjoining granite. I have since lost much of ray 
 faith in this supposition, since I have convinced myself that schistose structure is 
 not necessarily the result of aqueous sedimentation, but that cooling eruptive masses 
 under circumstances can assume a schistose form. * * * I am inclined to suppose 
 
 that these schists so intimately associated with massive diorite beds are a product of 
 their decomposition, under circumstances favoring the schistose arrangement of the 
 molecules, or, to speak in more definite terms, are a modified form of these eruptive 
 masses, and do not refer to former sedimentary deposits. 
 
 My examinations of the Marquette region, made at different times in 
 the summers of 1883, 1886, and 1887, have served to convince me thus 
 far of the correctness of the views of most of- the geologists who have 
 examined the region with regard to the inferior position of the rocks of 
 the greenstone-schist area to the remainder of the stratiform rocks. 
 They have also served to impress me strongly with the probable cor- 
 rectness of the view which would make at least some granitic rocks sub- 
 sequent in point of time to the greenstone schists themselves, since the 
 latter are so intricately penetrated by granitic bosses and dikes in their 
 more northern portions. 
 
 I have also seen enough to make me confident that the dike masses 
 which cut the greenstone schists of this area are of wholly subsequent 
 date to the schists, and indeed are equivalent in point of time to 
 those intruded sheets and masses which lie within the overlying de- 
 trital iron-bearing series. On the other hand, £ have seen some reason 
 to suspect that nearly all previous geologists have been mistaken in 
 considering the rocks of the greenstone- schist area as belonging within 
 the same great geological period as that which holds the remainder of 
 the stratiform rocks of the region. In other words, it thus far appears 
 to me that there is good reason to believe that these greenstone schists 
 along with the granites, gneisses, etc., form a portion of the basement 
 upon which the overlying detrital iron-bearing series was once horizon- 
 tally and unconform ably spread. That they do not constitute the con- 
 formably underlying basement beds of that series is suggested by a 
 glance at the map (PI. I), from which it will be seen that they do not 
 everywhere appear between the granite areas and the detrital rocks 
 themselves, the granite at times coming in contact with them, and again 
 with the higher stratiform horizons. But this anomalous arrangement 
 
 1 Geological Ileport on the Upper Peninsular of Michigan, exhibiting the progress of the work 
 
 from 1881 to 1884. 
 
20 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 might possibly be explained by the eruptive nature of the granite, 
 which, since eruptive, would come up indifferently at any horizon of 
 the rocks intruded by it. However, that the granite is not newer than 
 those stratified rocks which overlie the greenstone schists there appears 
 very excellent proof. At a number of points where the detrital beds, 
 which form the basement members of the iron-bearing series proper, 
 come in contact with the granite, they contain’ its debris in a very notable 
 fashion, while they are entirely devoid of granitic veins, such as occur 
 where the greenstone schists come into contact with the granite. If, 
 then, the granites are of one general age, it appears manifest that they 
 are newer than the greenstone schists, but older than the overlying 
 strata. Moreover, there are several points on the contact line between 
 the detrital rocks of the iron-bearing series and the underlying green- 
 stone schists, where a conglomerate is to be seen, in which are included 
 not only numerous granitic fragments, but also large sized pieces of the 
 greenstone schists themselves. 
 
 Since the occurrence of these basal conglomerates is a matter of so im- 
 portant a bearing on the geologic structure of this region, it is desira- 
 ble that the points of their occurrence should be briefly indicated here. 
 Beginning with the south side of the main, or southern area of the iron- 
 bearing series, indicated on the accompanying sketch map, it may be 
 noted in the first place that at several points along the contact line 
 in Secs. 1, 2, 3, 4, and 5, T. 47 N., R. 25 W., the basal quartzite of the 
 detrital series, which is in general made up almost completely of quartz 
 fragments cemented by a siliceous matrix, takes on a peculiar charac- 
 ter, containing at times a large quantity of pinkish orthoclase, along 
 with a good deal of sericitic mica. This peculiar rock was regarded by 
 Dr. Rominger as having been altered from the quartzite by its contact 
 with the more recently erupted granite. A study of the thin sections, 
 however, reveals the completely fragmental nature, not merely of the 
 quartz, but of the feldspar pieces, while the sericitic ingredient appears 
 to have arisen from an immediate alteration of the feldspar fragments. 
 These feldspathic fragments, as also the quartz mingled with them, are 
 of the kinds characteristic of granite, and, moreover, are entirely iden- 
 tical with those occurring in the granite with which this peculiar rock 
 is in contact. Southwest of Goose Lake, however, in Secs. 21 and 22, 
 T. 47, R. 26 W., there are much more obvious occurrences of gran- 
 itic debris. In the lower detritals of the iron-bearing series near the 
 southwest quarter of section 22 may be seen layers of fragmental quartz 
 slate holding seams of granitic pebbles; while in the southeast quarter 
 of the same section contacts are seen between the fragmental quartzite 
 and masses of the granite, the quartzite at the contact being crowded 
 with bowlders and fragmental material of all sizes derived from the 
 granite. It is not evident whether the granitic masses here seen are 
 brought to view by a fold of the strata, or are directly connected at 
 surface with the main granitic mass lying to the southeast of them, the 
 
IRVING.] 
 
 BASAL CONGLOMERATES NEAR MARQUETTE. 
 
 21 
 
 exact outlines of the areas occupied by different rocks in this vicinity 
 having never been traced. These occurrences were noted by Dr. Rom- 
 inger, 1 who also describes similar ones as obtaining in the southwest- 
 ern x>ortion of the same township. It should also be said that, at 
 numerous points along this line, the quartzite contains pebbly beds in 
 which the pebbles are of a quartzite whose microscopic features prove 
 to be those so well known as characteristic of the quartz of granite. 
 
 Turning now to the northern line of the same area we may note first 
 the conglomerate to be seen on the side of the so-called State Road, 
 running west from Marquette at a point near the west line of the SW. 
 J of the SE. J sec. 29, T. 48 R. 25 W. This is exactly on the line 
 between the greenstone- schist area and the area occupied by the detrital 
 rocks, which just here are thinly banded slates, standing vertical or 
 even overturned slightly so as to dip to the northward and to lie in gen- 
 eral conformity to the cleavage of the greenstohe schists immediately 
 north. These slates, whose lithological character is one very commonly 
 met with at the base of the iron-bearing series in many different por- 
 tions of the Lake Superior region, are proved by the thin sections to 
 be quite beyond question water-formed detritals and at the same time 
 to present a most striking contrast with the hornblendic and chloritic 
 greenstone schists lying immediately north of them. This contrast, 
 however, though very distinct in the thin section, is by no means so 
 pronounced in the hand-specimens which, though one sees that they are 
 of two different natures, might nevertheless be readily takeu to be all 
 of the same origin. At the point indicated the fragmental slates become 
 crowded with large and small fragments of granite, quartz, and green 
 schist, the quartz pebbles usually being of rather small size, while those 
 of granite, which are the most numerous, are well rounded and reach as 
 much as two feet in diameter. The green schist pebbles, on the other 
 hand, are not so plentiful, but are still abundant and of all sizes, from 
 the smallest particles up to pieces a foot across. The larger schist 
 pieces are somewhat rounded, but in the main they are all far less so 
 than the fragments of granite and quartz. The thin sections cut from 
 the matrix of the rock show that it is completely of a detrital nature. 
 On the north side of Teal Lake, at both eastern and western extremities, 
 are found other conglomerates, in one case holding only quartz pebbles, 
 and in the other case pebbles not only of quartz, but of greenish schists 
 as well. 
 
 Turning our attention now to the northern one of the two detrital 
 areas indicated on the sketch-map herewith (PI. I), I may note the oc- 
 currence at a number of points along its southern margin of conglom- 
 eratic layers of quartzite and sandstone, in which are contained peb- 
 bles of white quartz, which pebbles are at times identical in microscopic 
 and macroscopic appearance with the quartz of certain seams in the 
 greenish schists (as, for instance, on the west line of Sec. 20, T. 48 N., R. 
 
 1 Geol. Survey, Michigan, vol. 4, 1881, pp. 62, 63. 
 
22 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 . 
 
 27 W.), or with that of the granite (as, for instance, near the middle of 
 the south half of Sec. 17, T. 48 N., R. 26 W.), against which different 
 rocks the quartzites rest indifferent places. Near the middle of Sec. 21, 
 T. 48 N., R. 27 W., the quartzite, resting here against certain agglom- 
 erate green schists, contains not only fragments of quartz like that of 
 numerous seams in the green schists, but also pieces of the green schists 
 themselves, which in some cases are several inches in diameter. 
 
 But the most striking occurrences of basal conglomerates upon the 
 edges of this area of detrital rocks are those to be met with in the 
 northern and western portions of T. 49 N., R. 28 W. One of these places, 
 to which my attention was first drawn by Mr. C. E. Wright, the state 
 geologist of Michigan, is on the northwestern shore of Silver Lake, in 
 the SE. J of the Is W. J of Sec. 8. Rising abruptly all along the north- 
 ern side of this lake is a bold ridge of granite with which are associated 
 several kinds of schistose rocks, very prominent among which is a fine- 
 grained green schist entirely analogous in general appearance to the 
 greenstone schists which form the special subject of this paper. At 
 the particular point to which attention is now directed, this granite pro- 
 trudes in places into the lake in low, shelving ledges, facing which, and 
 lying within the cracks of which, is a black cherty slate. Following 
 the shore along to the southwestward from these exposures, the cherty 
 slate is found more largely developed, occupying a large hollow in the 
 surface of the granite, and becoming crowded with its fragments of all 
 sizes, from a fine detritus up to pieces two feet in length. These frag- 
 ments, though prevailingly subangular to angular in outline, generally 
 present some evidence of water- wearing. Many of them are quite 
 gneissoid in structure, while others are more granitic, two principal 
 phases being thus presented. The thin sections made from the speci- 
 mens selected on the ground as characterizing these two phases of peb- 
 bles, and also the granitic and gneissoid phases of the granite against 
 which the conglomerate rests, show the entire indentity of the frag- 
 ments and the massive granite. In addition to the granite fragments 
 are rarer ones of white quartz, these occasionally being of some size, 
 and others of a greenish schist entirely analogous to that green schist 
 which occurs here in situ along with the granite. The matrix of this 
 conglomerate is a dark gray to nearly black, carbonaceous, cherty slate, 
 which in the thin section shows a predominating quantity of a cherty, 
 chemically deposited silica, with which are mingled varying proportions 
 of fragmental material, this fragmental material being composed of 
 pieces of quartz and feldspar, and again, when the pieces become coarser, 
 of a granite in which these same minerals are attached to each other. 
 At times, as is so commonly the case among the cherty rocks of the 
 iron- bearing series generally, throughout the Lake Superior region, there 
 is a brecciated condition in this slaty matrix itself ; that is to say, irregu- 
 lar, angular pieces of the carbonaceous cherty material are cemented 
 together by a matrix of the same substance. Quite similar occurrences 
 
IRVING.] 
 
 AGE OF THE GRANITES, 
 
 23 
 
 are met with near the center of Sec. 19, of the same township, where 
 black cherty slate and quartzite lie upon the east and south flanks of a 
 bold hill of granite ; both slate and quartzite, and particularly the lat- 
 ter, being crowded with fragments of the granite, which range from 
 small pebbles up to pieces a foot or more in diameter, the smaller sized 
 pebbles being usually quite well rounded, while the larger fragments 
 are subangular to angular. 
 
 Such occurrences as these, when considered in connection with the 
 manner in which the granite penetrates the greenish schists and is in- 
 volved with them, seem to render necessary the belief that, while it is 
 plainly younger than the green schists, it is nevertheless greatly older 
 than the overlying detrital rocks ; and more than this, that when the 
 latter rocks were spread, the granites and greenstone schists together 
 had already suffered disturbance and deep denudation. It does not 
 appear possible to escape this conclusion by . supposing that, since 
 granite and greenstone schists are eruptives, they may have furnished 
 fragments to almost contemporaneous sedimentary deposits ; for, in 
 the first place, both the greenstone schists and the gneissoid granite 
 must have receiv'ed their schistosity before yielding the fragments. 
 Moreover, whatever may have been the depth at which the schistose 
 rocks were first formed, the granitic masses which intruded them, ac- 
 cording to all the later developments and doctrines of petrography, 
 must have been crystalized in depth, and must therefore have had re- 
 moved from over them great masses of materials before yielding frag- 
 ments to wave action. In this connection attention should be drawn 
 to the fact tbat there are evidently granitic rocks of two different ages 
 in the great granitic areas of the Marquette region ; because dikes of a 
 fine grained, reddish granite are frequently met with cutting the other 
 granite, which may be either gneissoid or not. These later granites, 
 which appear to be of relatively small extent compared with the main 
 mass, may perhaps have been even later in time of formation than the 
 detrital rocks themselves. It seems probable that to these later granitic 
 eruptions we should refer certain Tare quartz-porphyry dikes, and such 
 very rare granitic dikes as that which is seen near Metropolitan, in the 
 Felch Mountain district, intersecting a ferruginous schist of the iron- 
 bearing series itself. 
 
 On the whole, then, accepting Prof. Williams’s conclusions as to the 
 surface origin of most of the greenstone schists of the Marquette 
 region, I should suppose that, after the accumulation of these rocks to 
 the thickness of several thousand feet, they were intruded by granitic 
 bosses. These bosses perhaps may have been merely softened portions 
 of the underlying gueissic basement, which indeed may be represented 
 in an unaltered condition in portions of the granitic areas themselves, 
 for all that has yet been determined to the # contrary. Subsequent 
 mountain-making movements brought about the folding and altera- 
 tion of these enormous sheets of eruptive material, now represented by 
 
24 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 the greenstone schists. Following this was the great denudation 
 which brought to light the previously buried granitic masses. This 
 erosion was followed in turn by the accumulation in the usual horizon- 
 tal position of the iron-bearing detrital series, whose folding and erosion 
 were still later processes. And yet this folding and erosion all pre- 
 ceded the deposition of the horizontal Cambrian sandstones of the 
 region. 
 
 The entire similarity which is shown by Prof. Williams to obtain be- 
 tween the great dikes of diabasic greenstone which traverse the green- 
 stone schist area, and the sheets of eruptive greenstone which are in- 
 cluded within the iron-bearing series, furnishes a further confirmation 
 of these conclusions. For the latter greenstones are in large measure 
 directly interstratified with the sedimentary layers of the iron-bearing 
 series, following the bending of its layers; so that even if these green- 
 stones are in the nature of intruded sheets, it seems necessary to be- 
 lieve that their intrusion took place before the folding of the iron-bear- 
 ing series. Now, the corresponding dikes in the greenstone-schist area 
 were evidently intruded subsequent to the production of the schis- 
 tosity of the intruded rocks. If, then, these are facts, the time when 
 the iron-bearing series was folded was very much subsequent to that 
 time at which the greenstone schists received their schistosity. It has 
 been mentioned that the schistose structure of these greenstones at 
 times corresponds with the bedding structure of the iron-bearing 
 series. But quite frequently there is no such correspondence, the beds 
 of the latter series being noticeably at relatively lower angles when 
 compared with the vertical 1 schistose structures of the greenstone 
 schists themselves. 
 
 Such correspondence in some places and lack of correspondence in 
 others are easily enough explicable upon the views that I have ad- 
 vanced. However, there is good reason to think that at the time of the 
 folding of the iron-bearing series, the greenstone schists received a sec- 
 ond squeezing, which developed further alterations and further schis- 
 tosity. The later dikes just alluded to as penetrating the green schists 
 are at times rendered somewhat schistose, though far less markedly so 
 than are the rocks which they intrude. The same is true with the green- 
 stones that are intercalated in the iron-bearing series, where somewhat 
 schistose phases are found. The structure of these last-named schis- 
 tose phases, as also the occasional slaty cleavage seen in the detrital 
 layers of the iron-bearing series, where it is very strongly folded, cor- 
 respond in general direction, as would be expected, with the schistose 
 structure of the green stone- schist areas. 
 
 The geology of that portion of the Menominee region which has been 
 especially under study in the present connection, is indicated by the 
 outline map, Plate II. Here, again, we find a series of detrital iron- 
 bearing rocks, lying between great areas of granite and gneiss. The 
 iron-bearing rocks are generally quite closely like those of the Mar- 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
T. 38 N 
 
 R. UFOLOGICAL SURVEY- 
 
 Antoine 
 
 ^.0 liapin Myy_ 
 l Mquntam - 
 
 Yieinne: 
 
 SR# 
 
 *. " v , «\ t, V%f. >- 
 
 WimiM 
 
 ARCHEAN. 
 
 Granite and Gneiss. Greenstone Schists 
 
 OUTLINE GEOLOGICAL MAP C 
 
 Compiled, bv R.D. Irving from maps by T.B.B rooks, 
 
 Seal 
 
 .0 .3 _ 
 
ALGONKIAN 
 
 Iron Bearing Series. 
 
 •tritals, Limestones & Femicjinmis . 
 Sri lists.) 
 
 A i 
 
 CAMBRIAN. 
 
 j A_ y 
 
 Potsdam Sandstone . 
 
 | 
 
 THE MENOMINEE IRON REGION. 
 
 AVriijht and ('.Roniinger and lrom original observations. 
 
 f miles. 
 
 .6 ,9 
 
 080 
 
 T.39N. 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
lKVTN'G,] 
 
 GREENSTONE SCHISTS ON THE MENOMINEE. 
 
 25 
 
 quette region, the only important differences being the very great rar- 
 ity of greenstone intrusions, and the very much more closely crumpled 
 condition which the rocks here present. In the same region are two 
 belts of greenstone schists closely analogous in general appearance 
 with those of the Marquette region. The southern one of these borders 
 for a long distance the southern granite area, separating the granite 
 from the detrital rocks further north. The inclination of the schistosity 
 of the greenstone schists is almost vertical, there being generally a 
 slight southern departure from verticality. Very high southern dips, 
 often approaching verticality, also prevail among the layers of the de- 
 trital succession itself, although here frequently occur reverse dips to 
 the northward, often at a flatter angle. 
 
 The first geologists who appear to have noted the Menominee rocks 
 are Foster and Whitney and Charles Whittlesey, as quoted in Foster 
 and Whitney’s work. 1 By these writers all of the Menominee strati- 
 form rocks, so far as they were encountered in the rapid trips by canoes, 
 which were at that time the only means of traversing the country, 
 were classed together under the general name of Azoic slates. How- 
 ever, the exposures of greenstone schists, which are met with at Twin 
 Falls, Upper (Big) and Lower (Little) Quinnesec Falls and Sturgeon 
 Falls, appear to be directly referred to as intercalations of “ Azoic 
 slates and traps ; ” so that, while no opinion was expressed as to their 
 stratigraphic relations to the other rocks of the region — beyond what is 
 indicated in general statements as to the greater recency of all the 
 granitic masses of the region as compared with the schistose and slaty 
 rocks — it appears plain that these geologists looked upon the rocks 
 now included under the term of greenstone schists as partly eruptive 
 and partly sedimentary. 
 
 The same conclusion as to the origin of these rocks appears to have 
 been reached by Gredner, who published an account of this region in 
 I860, 2 after having been some time on the ground as an assistant to 
 Prof. R. Pumpelly in a private economic examination of the lands of 
 the Lake Superior Ship Canal Company. On account of the slight de- 
 parture from verticality towards the south; on account of the schistose 
 structure of the rocks exposed at the several falls of the Menominee, 
 which rocks he describes under the general term of “ Dioritic Series’ 
 and “Talcky Clay Slate,” and because of the prevalence of similar 
 southern dips among the detrital iron-bearing rocks farther north, 
 Credner considers the former rocks as constituting the highest portion 
 of the entire succession of the region. That there existed to the south 
 of these rocks another mass of granite does not appear to have been 
 realized by Credner. 
 
 T. B. Brooks, who followed Credner in the Menominee region and 
 
 * Geological Survey of the Lake Superior Land District, vol. 2, pp. 24-31. See also general soctlon 
 of the Lake Superior region in atlas to the same volume. 
 
 2 Die vorsilurischen Gebilde dor oberen Halbinsel von Michigan in Nord-Amorika. Zeitschr. 
 Deutsch. geol. Gesell., Berlin, 18G9, vol. 21, pp. 516-554. 
 
26 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 . 
 
 who published a brief account in the reports of the Geological Survey of 
 Michigan 1 , appears to have agreed with that geologist with regard to 
 the relatively high position in the series of the greenstone schists of 
 the Menominee River. Subsequently the same geologist, assisted by 
 0. E. Wright, was engaged in a more minute examination of this 
 region on the part of the Wisconsin State Geological Survey, publish- 
 ing a somewhat elaborate report in 1880. 2 In this report very many 
 more facts are given than were ever known before, all exposures seen 
 being very accurately and carefully indicated upon the accompanying 
 maps. This detailed work, however, does not appear to have altered 
 Brooks’s opinion as to the relatively high position in the Menominee 
 series of the greenstone schists now especially under consideration, 
 although it appears that he would now correlate them with still higher 
 layers of the Marquette series rather than with those to which he 
 had previously referred them. As to the origin of the greenstone 
 schists, Brooks would seem to have regarded them at first as all sedi- 
 mentary; at all events when the Michigan report referred to was 
 written. 3 Later, however, he appears to have been disposed to separate 
 from the rest certain diabases as eruptive, thus coming nearly to the 
 same conclusion as that reached by Credner. 4 To convey Brooks’s con- 
 ception of the structure of this region more clearly, there are given here 
 two sections, constructed from general sections given by him upon 
 Plates 27 and 29 of the atlas to the Geology of Wisconsin. The granitic 
 
 jswr JV"JE. 
 
 Fig. 1 . Hypothetical section of the Menominee region in the vicinity of Quinnesec, according to 
 Brooks; I, Sericitic slates; II, quartzite ; V, limestone; VI, the great iron horizon; XIV, quartzite ; 
 XV to XIX, greenstone schists, etc. ; XX, Huronian granite; P, Potsdam sandstone. Scale 13,000 
 feet to the inch. 
 
 and gneissic rocks to the north Brooks regarded as having formed part 
 of the ancient Laurentian basement upon which all of the slates and 
 schists were subsequently piled. From this northern granite to the 
 granite on the south side of the Menominee he looked upon the entire 
 succession as an ascending one, though admitting certain bowings of 
 the strata. The southern granite, as to whose sedimentary or eruptive 
 origin he appears to have been doubtful, he places as the summit mem- 
 ber of the Huronian series. The entire succession he divides into three 
 portions, beginning below or to the north, as follows : Lower Huronian, 
 
 1 Geol. Michigan, vol. 1, 1873, pp. 157-182. See also atlas to the same, PI. 4. 
 
 2 Geol. Wisconsin, vol. 3, 1880, pp. 430-663 ; also atlas, Pis. 28-30. 
 
 8 Geol. Michigan, vol. 1, 1873. 
 
 4 Geol. Wisconsin, vol. 3, 1880, p. 521. 
 
IRVING.} 
 
 OBSERVATIONS OF BROOKS AND ROMINGER. 
 
 27 
 
 5,200 feet ; Middle Huronian, 3,100 feet; Upper Huronian, 10,700 feet; 
 making in all a maximum thickness of 19,000 feet beneath the upper or 
 southern granite. The surface distribution of the uppermost of these 
 three divisions corresponds almost exactly with the areas of greenstone 
 schists indicated upon the outline map herewith (PI. II). The more north* 
 
 HURONIAN 
 
 Fig. 2. Hypothetical section of the Menominee region in the vicinity of Twin Falls, according to 
 Brooks. Scale 13,000 feet to the inch. Letters and shadings have the same significations as in Fig. 1. 
 
 ern area of greenstone schists, namely, that which is sectioned by the 
 Menominee river at Twin Falls, is made on Brooks’s structural sketches 
 to be brought to view by a synclinal depression of tbe strata. For this 
 view of the structure of the region there never was any other support 
 than the very slight departure from verticality towards the south of 
 the schistose structure of the southern greenstone schists and a pre- 
 vailing similar inclination in the detrital iron bearing series proper. 
 No contacts of the different kinds of rocks were observed to support 
 Brooks’s hypotheses as to the relatively high position of the greenstone 
 schists and southern granite, between which and the other stratiform 
 rocks there is indeed usually a wide belt of country without exposures. 
 On the other hand, the extraordinary similarity of these greenstone 
 schists to those which Brooks regarded as underlying the entire 
 Marquette series appears to have been disregarded, as also was the 
 complete similarity between the northern and southern granites, and 
 again between the contact of the southern granite with the green- 
 stone schists next to it, and the corresponding contact in the Marquette 
 region. 
 
 Itominger, who followed Brooks in the Menominee region in 1880 
 and published an account of his observations in 1881, appears 1 to have 
 realized very vividly the difficulties met with in accepting Brooks’s 
 structural hypothesis. He represents all of the greenstone schists of 
 the region as belonging at the base of the entire stratiform series, and 
 as equivalent in position and nature with the similar rocks of the Mar- 
 quette region. The northern and southern granites Kominger looks 
 upon as the same, and as intrusives of a date later than the accumulation 
 of the entire stratiform succession. As to origin, he evidently looked 
 upon the greenstone schists as altered sedimentaries, assigning the 
 relatively great alteration, which on this view they must be assumed 
 to have undergone, to the action of the later granitic bosses; in which 
 
 •Geol. Survey Michigan, vol. 4, 1881, pp. 157-241. 
 
28 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 view he fails quite to explain, as he does in the case of the Marquette 
 region, how the southern granite of the Menominee area should have 
 produced so great alterations, while that on the north comes in contact 
 with wholly unaltered detrital rocks, to which moreover, as Brooks had 
 previously shown, it furnishes an abundance of detrital material. Un- 
 fortunately, though describing carefully very many exposures not re- 
 corded on Brooks’s map, Bominger gives no sections indicative of his 
 views as to structure. Just what his ideas were in this respect it is 
 not easy to make out from his descriptions, but it appears evident that 
 with him the greenstone schists lie at the base of the succession 5 that 
 they are next succeeded in order by those slates which lie about Lake 
 Hanbury; that these are succeeded by the great ore horizon, and this 
 by the great limestone bed of the region with a thickness of a thousand 
 feet and more. Thus he reverses entirely the succession as given by 
 Brooks, and as it appears in nature so far as the limestone and ore 
 belts are concerned. What strati graphical position Rominger would 
 give to those great masses of quartzite which lie adjacent to the northern 
 granite in Menominee belt I have not been able to understand distinctly 
 from his descriptions. The Twin Falls greenstone schists he would 
 place along with the Quiunesec series at the base of the entire succes- 
 sion, bringing them to the surface by an anticlinal instead of a syn- 
 clinal fold, such as is resorted to by Brooks. The following paragraphs 
 are quoted from Rominger, 1 as indicative of his views upon these points : 
 
 A superposition of the diorite formation on the Lake Hanbury rock series, which 
 adjoins in the whole length of the Menominee valley from the upper Quiunesec Falls 
 to the Sturgeon Falls, asserted by Major Brooks, is not observable ; the nearly verti- 
 cal strata of both formations are even never seen in contact. There is always 
 quite a large covered interval between them. The nearest exposures of the two groups 
 are observable in Sec. 26, T. 39, R. 29, where, in the center of the section, a hill is formed 
 of the vertical ledges of ferrugino-siliceous flagstones and slaty beds representing the 
 Lake Hanbury series, and about two or three hundred steps from these exposures we 
 find on the south side of the road to Menominee small hillocks of diorite. * * * 
 
 My reasons for holding the dioritic rocks south of the iron formation as older 
 than the latter are based on the lithological similarity of this formation with 
 the dioritic group of the Marquette district and on the degree of metamorphism ex- 
 hibited by the two groups, the dioritic and the iron-bearing. In the great succession 
 of strata commencing with the Hanbury slate group and upward we rarely find a 
 bed so much altered that its sedimentary structure is altogether obsolesced, and the 
 majority of the strata shows it very plain, while in the dioritic rocks, considered to be 
 the younger, a stratified structure is also recognizable, but not one of these thousands 
 of feet of ledges exhibits its original sedimentary lamination with any degree of dis- 
 tinctness like the others ; they have evidently been transformed under cooperation 
 of heat and partially brought into a plastic condition, which is shown by the ex- 
 treme corrugation and mode of intermixture of those rock masses, of which effects the 
 other rock groups do not exhibit near as high a degree. It would be very strange, 
 then, if the lowest beds nearest to the focus of the central heat should have been so 
 much less affected by these altering influences than those pretended to be the higher 
 upper strata of the rock crust. One might object : If the diorites are the older beds, 
 why don’t we find them just as well developed on the north side of the upheavedbeds 
 between the quartzite and the granite ? The saudy and conglomeratic nature of 
 
 1 Geol. Survey Michigan, vol. 4. 1881, pp. 208-210. 
 
IRVING.] 
 
 OBSERVATIONS OF ROMINGER AND IRVING. 
 
 29 
 
 many of the strata of the quartzite and iron formation proves them to be shore depos- 
 its, while the dioritic group consists only of the finer material of deep sea deposits, 
 which explains the point in question. Moreover, the dioritic rocks are not altogether 
 missing on the north side of the ore-formation, as we can see by the occurrence of the 
 6-mile-long chain of diorite extending eastward from the Twin Falls. A similar dis- 
 crepancy between the rocks underlying the ore-formation on the two opposite sides 
 of its exposure is seen in the Negaunee district. On the south margin, at the Cas- 
 cade and Palmer mines, it rests directly on the granite, while on the northern expo- 
 sures the diorite underlies it in great thickness. 
 
 The equal dip of the strata to the south in these adjoining formations is not neces- 
 sarily a proof of the younger age of the most southern beds. The whole succession is 
 so near to a vertical position that in many instances it has to be left uncertain which 
 way they dip, but suppose their dip is conformably to the south ; the upheaval of the 
 diorites by the eruption of the still more southern granite masses pushing the whole 
 incumbent rock-series north until all tipped over is the hypothesis by which I explain 
 the order in the succession of beds as an inverted one, the seemingly lowest beds being 
 actually the youngest. 
 
 In my own studies in the Menominee region, made in the summers of 
 1883 and 1885, 1 became early impressed with the close similarity be- 
 tween the greenstone schists of the Menominee River and those which 
 underlie the iron-bearing series of Marquette ; with the entire similar- 
 ity between the rest of the stratiform rocks of the region and those of 
 the Marquette district ; with the essential identity in character of the 
 granite areas lying respectively on the northern and southern sides of 
 the Menominee River; with the granitic intrusions met with in the green- 
 stone schists bordering the southern granite, and with the striking con- 
 trast between the nature of this contact and that of the northern gran- 
 ite with the detrital rocks which border it to the south. In the latter 
 case the granite, instead of sending intrusions into the rocks which 
 rest against it, has furnished fragments to them, as may be most beau- 
 tifully seen at the Falls of Sturgeon, Sturgeon River, on the eastern side 
 of Sec. 8, T. 39, R. 28 W., Michigan. 1 These considerations naturally 
 
 1 For previous descriptions of the striking occurrences at the Falls of Sturgeon, Sturgeon River, 
 see Credner in “Die vorsilurischen Gebilde der oberen Halbinsel von Michigan,” Zeitschrift der 
 Deutschen geologischen Gesellsehaft. vol. 21, 1869, p. 521, et seq. ; also T. B. Brooks, in Geol. Wisconsin 
 vol. 3, 1880, pp. 467, 468, and Atlas, PI. 38 ; also, see Rominger, Geol. Michigan, vol. 4, p. 192. The 
 granitic fragments at this place occur in a fine-grained slaty rock, in which there is a great deal of 
 gericitic material, which at times gives the slate somewhat the look of a crystalline schist. This fact, 
 along with the slight inclination from the vertical towards the north, and therefore towards the gran- 
 ite, which is so largely exposed farther up the stream, led Credner to include these conglomeratic lay- 
 ers, along with the granite, as Laurentian, the great quartzite mass farther south being taken by him 
 as the basement member of the Huronian. Brooks, however, objects to this conclusion, considering 
 that the conglomerates to be seen at this place are genuinely basal conglomerates, and that they form 
 the lowest portion of the Huronian region. To support this view, Brooks draws attention to the fre- 
 quent arenaceous nature of the conglomeratic slates-, their ripple-marked surfaces; their generally 
 little altered appearance ; their parallelism of strike with the admitted Huronian beds farther south, 
 and the lack of parallelism between this strike and such structures as is to be seen in tho granitic and 
 gneissic rocks on the north. Rominger’s description corresponds with that of Brooks, except that he 
 seems to describe a granitic mass or sheet as occurring interleaved with the conglomerates themselves, 
 a statement for which, in my examinations, I could find no support whatever. Rominger, however, 
 to whom the greater recency of all the granite as compared with all the stratiform rocks was an ac- 
 cepted conclusion, explains the occurrences as he saw them by the singular supposition that “we have 
 here evidently a series of sedimentary beds, deposited on a granitic substratum, which, during the up- 
 heaval, became wedged in between the plastic granite mass, tilting and overlapping them locally so as 
 to appear as tho lower beds,” thus making the same granite yield fragments to tho sedimentaries, and 
 subsequently intrude them, It should bo said that the examinations of tho sovoral geologists were 
 
30 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 | BULL. 62. 
 
 led me to the conclusion that the whole structure in this district is sim- 
 ilar to that already described as obtaining in the Marquette region, 
 namely, that the granitic masses had intruded themselves in the shape 
 of great bosses into rocks now represented by the greenstone schists, 
 after which followed a protracted period of disturbance and denudation 
 before the deposition of the overlying detrital and iron-bearing rocks 
 of the region. Taking Major Brooks’s detailed map of the Menominee 
 district, published in the atlas of the Wisconsin survey, I platted upon 
 it all of the exposures described by Rominger and not mapped by 
 Brooks, which exposures amount in all to a large number. Examining, 
 then, the more important of the exposures of the region, I encountered 
 still others, which were also platted upon the same map. Two sections 
 were then constructed across the district from southwest to northeast, 
 upon which wereplatted all of these exposures, with their dips ; and it 
 should be said that very many new facts in this direction have been 
 developed of late years by mining. 
 
 H U R O A FT I -A 1ST 
 
 iS'.W G Sch, / TeTcd E D G c C D E D C D~i D C B COED C B ^ G 
 
 Fig. 3. Hypothetical section of the Menominee region in the vicinity of Quinnesec Valley, accord- 
 ing to R. D. Irving. A, basal sericitic quartz slates ; B, quartzite; C, limestone; D. iron horizon ; E, 
 slates and quartzites; G, granite and Sch., schists of the Laurentian. Scale, 13,000 feet to the inch. 
 
 It has thus become evident that a structure such as is indicated in 
 the accompanying Fig. 3 would not only coincide with the recorded 
 facts as well as the sections of Brooks above given, but very much bet- 
 ter than those. 
 
 made ■without the study of thin sections hf the slaty rocks here exposed. When examined microscopi- 
 cally, these rocks show their completely fragmental nature, all the alteration that they have under- 
 gone having been in the nature of a metasomatic development of mica flakes. Both hand specimens 
 and thin sections of these slates, moreover, show a most striking similarity between them and the 
 slaty rocks which frequently lie at the base of the Penokee series of northern Wisconsin and Michi- 
 gan, where they are often in contact with granitic rocks, of which they hold fragments. Similar slates 
 are met with in a number of places at the base ox the iron-bearing series of the Marquette region. As 
 seen at the Sturgeon Falls, these slates are at times fine grained and thinly laminated, arenaceous and 
 sericitic, and again more closely grained and of a vitreous quartzitic appearance, in which cases the 
 predominating quartz fragments have been cemented together by secondary enlargement. Their entire 
 ackof anything like metamorphism is perfectly plain, even without the examination of the thin sec- 
 tion, to any one who has studied many sections of such rocks from the Lake Superior country. The 
 pebbles in these slates are arranged in bands, with intervening less pebbly or non-pebbly portions, 
 which portions are the ones which show particularly the ripple-marked surfaces. The pebbles are in 
 the main of a pinkish granite and gneiss, wholly identical with the mass of granite and gneiss against 
 which they lie, but include also a smaller number of pieces of white quart z and of a fine-grained green- 
 stone or greenstone schist. Entirely similar quartz occurs in seams in the granite close by, as do also 
 masses of greenstone and greenstone schist. Net only these pebbles, but the whole make-up of the 
 finer portion of the rock, make it entirely evident to me that we have here to do with a detritus derived 
 by water action from the granitic and gneissic area immediately to the north. The slight inclination 
 away from the vertical towards the granite which these conglomeratic slates sometimes show is, of 
 course, no argument against their having been deposited upon that granite as a substratum. 
 
THE GREENSTONE SCHIST AREAS OF THE MENOMINEE AND 
 MARQUETTE DISTRICTS, MICHIGAN. 
 
 By George Huntington Williams. 
 
 INTRODUCTION. 
 
 This memoir is intended as a contribution to the subject of dynamic 
 or regional metamorphism. It contains the results of a careful study, 
 both in the field and in the laboratory, of an extensive series of erup- 
 tive rocks, for the most part of basic character. Although the original 
 character of these rocks is still evident, they are to a large extent 
 cleavable, and the production of this secondary feature has been 
 accompanied by more or less extensive chemical and structural altera- 
 tions. 
 
 It is the aim of this paper to trace each of the rock types repre- 
 sented within the areas studied from its least altered to its most 
 altered form, and to discuss what may have been the agencies which 
 produced the changes noticed. 
 
 The rocks selected as likely to throw additional light upon the meta- 
 morphism of eruptive masses are so-called i( greenstones ” and a green- 
 stone schists,” which, in association with certain more acid types, cover 
 extensive districts on the south shore of Lake Superior, where they 
 lie immediately beneath the iron-bearing strata. Two distinct and 
 sharply defined areas of these rocks were choseu as typical of the 
 whole formation. Particulars regarding their geographical positions 
 and their geological relationships have already been given by Professor 
 Irving in his preliminary note. In the first area, situated on the 
 Menominee River, the eruptive character of* the greenstones and green- 
 stone schists is plainly evident ; within the second area, near the city 
 of Marquette, the original character of the rocks is much less apparent. 
 
 The investigations, the results of which are embodied in this mem- 
 oir, were first suggested to me in the spring of 1885 by the late Prof. 
 R. I). Irving, while he was in charge of the Lake Superior division of 
 the U. S. Geological Survey. Their aim was to discover, if possible, 
 the origin of the greenstone schists of the Lake Superior region, and 
 at the same time to afford a contribution to our knowledge of the meta- 
 morphism of basic eruptive rocks in general. In the latter sense they 
 form a continuation of the writer’s earlier studies of the less altered 
 gabbros occurring near Baltimore, Maryland. 1 
 
 1 Bull. U. S. Geol. Survey, No. 28, 1886, 
 
 31 
 
32 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 Three weeks of the field season of 1885 were spent in the Menomi- 
 nee Valley, and four weeks of 1886 in the neighborhood of Marquette. 
 During this time, with the assistance of Prof. W. S. Bayley, the rocks 
 were examined in the field, and ample material was collected for their 
 laboratory study, which was carried on at the Johns Hopkins Uni- 
 versity, Baltimore, Maryland, during the winters of 1885-’86 and 1886- 
 ’87, at such times as could be spared from regular university duties. 
 The entire investigation has been conducted under the auspices of 
 Professor Irving, for whose uniform kindness and constant readiness to 
 supply every facility for the work I gladly take this opportunity of 
 expressing my sense of deep obligation. My thanks are also due to 
 Maj. T. B. Brooks and to Prof. Raphael Pumpelley for the loan of 
 microscopic sections of the Marquette and Menominee rocks, prepared 
 during the course of the Wisconsin State Geological Survey ; and to 
 Mr. Andrew 0. Lawson, Ph. D., lately of the Canadian Geological Sur- 
 vey, for the opportunity to make a comparative study of closely allied 
 rocks from the Lake of the Woods and the Rainy Lake regions. 
 
 I feel that no especial apology is needed for the constant use through- 
 out this paper of the term 44 greenstone.” An opinion prevails that this 
 word is antiquated and not consistent with the scientific accuracy now 
 obtainable. The very indefiniteness of this designation, however, con- 
 stitutes its chief value. It is essentially a field term, such as it is not 
 only desirable but absolutely necessary to employ. It is often impos- 
 sible to state with certainty in the field whether a given basic massive 
 rock is a gabbro, a diabase, or a diorite ; indeed, where such masses have 
 undergone extensive metamorphism, as in the regions here studied, even 
 the most careful microscopical and chemical investigation may prove 
 inadequate to disclose what was the original form. Wherever accurate 
 diagnosis was possible, correspondingly definite terms have always 
 been employed ; but for use in the field or where the processes of alter- 
 ation have obscured the original character of the rock beyond recogni- 
 tion, an intentionally indefinite designation is necessary. For such a 
 purpose it is believed that no term is better fitted than the ancient and 
 much abused ‘‘greenstone.” 
 
 For convenient reference the specimen numbers belonging to the col- 
 lections of the Lake Superior division of the U. S. Geological Survey 
 are here appended. 
 
 1. Menominee Valley 
 
 Sturgeon Falls 
 
 Little Quinnesec Falls 
 Big Quinnesec Falls. .. 
 
 Horse Race 
 
 Four Foot Falls 
 
 Twin Falls 
 
 2. Marquette region 
 
 Marquette area 
 
 Negaunoe area .. 
 
 11000-11196 
 
 11153-11174 
 
 11000 - 11048 ; 11098-11103 
 11049-11085 
 
 11086 - 11096 ; 11182-11196 
 
 11142 - 11152 ; 11175-11181 
 
 11120-11141 
 
 11610-11864 
 
 11610-11734 
 
 11735-11812 
 
 Northern area 
 
 3. Agglomerates of Deer Lake 
 
 11813-11864 
 
 12023-12058 
 
WILLIAMS.] 
 
 INTRODUCTION. 
 
 33 
 
 The material embodied in the present paper will be arranged in three 
 separate divisions. 
 
 1. In chapter one the importance of the service which the microscope 
 is capable of rendering toward the solution of the questions of archaean 
 geology will be indicated and a summary presented of the chief results 
 already obtained by various workers in this field. 
 
 2. In chapters two, three, four, and five the observations collected 
 during an extended study of the rocks of the two areas selected will 
 be given in detail. 
 
 3. In chapter six a connected discussion of these results will be at- 
 tempted, and a comparison of them with those reached by other observ- 
 ers, as enumerated in chapter one, will be made. 
 
 Bull. 62 3 
 
CHAPTER I. 
 
 PRESENT STATE OF OUR KNOWLEDGE REGARDING THE META- 
 MORP.HISM OF ERUPTIVE ROCKS . 1 
 
 VALUE OF THE MICROSCOPE IN THE STUDY OF METAMORPHISM. 
 
 In comparison with the results which have been obtained during 
 nearly a century of patient research among sedimentary deposits, 
 the progress thus far made in the domain of archean geology ap- 
 pears small. Theories of the origin of theso-called crystalline schists 
 are almost as numerous as the investigators who have examined them, 
 and yet the more extensive and critical the studies of these rocks 
 become the more obscure and anomalous do they appear. So varied 
 are the facts which Nature presents to the observer in the oldest rocks 
 of the planet that the conviction is soon reached that no single hypoth- 
 esis or explanation can account for them. It is therefore from no lack 
 of interest attaching to the study of pre-fossiliferous rocks that they 
 have heretofore yielded so little fruit, but rather from the insurmount- 
 able difficulties which have stood in the way of their satisfactory inves- 
 tigation. That the study of fossils has made up so large a part of what 
 has been known as geology is the result rather of necessity than of 
 choice. The lack of exact and delicate methods of lithological research 
 has confined the attention of investigators to those formations where 
 lithological characters are of little value on account of the presence 
 of other and more certain guides. The basement underlying all of the 
 fossiliferous rocks has, therefore, remained well-nigh a terra incognita, 
 because there seemed to be no available means of exploring it. 
 
 The recent multiplication of refined methods for the investigation 
 of crystalline rocks, however, has opened an almost new field of geo- 
 logical inquiry. The difficult and obscure problems here presented 
 may now be attacked by truly scientific methods. The prophecies 
 which Hermann Vogelsang made in 1867 2 for the new departure in 
 geology have been more than realized within the last twenty years. 
 The almost new science of petrography may be said to have proved 
 itself capable of rendering, in the study of the crystalline rocks, a serv- 
 ice equal to that which paleontology has already given in the de- 
 ciphering and correlating of the fossiliferous strata. 
 
 1 This chapter was written as it now stands, excepting an occasional foot note, in 1887. 
 
 2 Die Philosophic der Geologic, Pt. 3, Moderne Geologic oder mikroskopischc Gesteinsstudien. 
 
 34 
 
. williams.] DEVELOPMENT OF MICROSCOPICAL PETROGRAPHY. 
 
 35 
 
 Petrography, in its rapid development since the introduction of the 
 microscope, has already passed through two distinct periods and is 
 now entering upon a third and most important stage. At first methods 
 had to be perfected for identifying the various constituents of crystal- 
 line rocks. During this stage the science was purely mineralogical, 
 although its methods were necessarily somewhat different, both in their 
 nature and in their application, from those of ordinary mineralogy. The 
 attainment of this end required the study of a vast amount of material 
 wholly without reference to its geological significance. 1 
 
 The second period in the development of petrography was occupied 
 with the investigation of practically unaltered rock-types, i. e., of rocks 
 in which the miuerals and structure produced by their original solidifi- 
 cation are still readily discernible. It has been found from such studies 
 that the relationship of the component minerals to one another, or rock- 
 structure, expresses, to a large degree, the circumstances under which 
 the original solidification took place, and hence the importance of the 
 second stage in the development of modern petrography. 
 
 The most important problems presented by an unaltered massive or 
 igneous rock relate to (1) its chemical composition and (2) to the con- 
 ditions under which it was formed. The composition expresses itself, 
 in a general way, in the nature of the component minerals, while phys- 
 ical conditions attendant upon the formation of the rock may be traced 
 in its structure. Each of these has therefore been, in turn, the partic- 
 ular object aimed at during the first two periods of petrographical re 
 search. 
 
 But if petrography were able to solve satisfactorily all the problems 
 presented by the unaltered massive rocks, it would even then be pre- 
 pared only to commence its most difficult and most important mission. 
 Rocks are in reality far from being the dead, inert, stationary masses 
 which they appear to the ordinary observer. The fascinating study of 
 chemical geology, especially when aided by the microscope, shows them 
 to be in a state of almost constant change. It is true that some of the 
 oldest rocks seem to have suffered hardly any alteration since they 
 were first formed, but most of them are ever active laboratories where 
 old products are being pulled to pieces and new ones built up. The 
 tracing out cf such changes is an important aim of petrography in its 
 present stage. 
 
 The student at the microscope wonders at the minute bubbles which 
 he so often finds inclosed in the little cavities in quartz. So delicately 
 are they poised that they are sensitive to all the slight oscillations of 
 temperature that constantly pass through the microscopic section, and 
 the little prisoners keep up a never-ending movement, as though beat- 
 
 ’Tlio writer lias given an account of the development of these methods in a small pamphlet, entitled 
 “Modern Petrography,” published as No. 1 of the Monographs of Education, by Heath & Co., of 
 
 Boston. 
 
36 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULU 62 . 
 
 ing against every side of their narrow cell in the vain search for an 
 exit. Scarcely less delicate seems to be the equipoise between the va- 
 rious chemical compounds in the earth’s crust and the surrounding 
 physical conditions under which they exist. Like the constant changes 
 of temperature which pass through the slide are the changes in physi- 
 cal conditions to which a rock-mass is subjected. With these comes a 
 state of more or less unstable equilibrium to the chemical compounds, 
 and, like the vibrations of the bubble, molecular movements and re- 
 arrangements result. 
 
 There are two distinct kinds of alteration which take place in a solid 
 rock-mass, dependent, of course, on the nature of the changed physical 
 conditions. These are : , - 
 
 (1) Metamorphism ; or the passage, under circumstances of high tem- 
 perature or pressure, or both, of less crystalline into more crystalline 
 compounds; or the change of minerals into others, not less crystalline 
 or insoluble than themselves. 
 
 (2) Decomposition or weathering ; the passage, under ordinary at- 
 mospheric conditions, of crystalline rock constituents into compounds 
 less crystalline and more soluble than themselves. This is accomplished 
 generally by hydration or carbonatization. 
 
 Both of these processes are frequently seen to have gone on in suc- 
 cession in the same rock-mass, the latter more or less completely ef- 
 facing the effects of the former. While distinct, both processes agree 
 in being atomic and molecular rearrangements in a solid mass, necessi- 
 tated by some change in external conditions. The differences in these 
 conditions, however, produce widely different results; and all of these 
 again are essentially different from those produced by the solidification 
 of a liquid magma. 
 
 The student of the crystalline rocks can distinguish in a general 
 way four classes of constituent minerals, and this is true in spite 
 of the fact that the same species may be represented in two or more of 
 these classes. 
 
 (1) Original minerals of the acid rocks, formed by solidification of a 
 magma in a state of aqueo-igneous fusion or by the aid of mineral- 
 izers ; e. g., quartz, orthoclase, mica, zircon, etc. 
 
 (2) Original minerals of the basic rocks, formed from a state of dry 
 fusion; e. g., plagioclase, augite, olivine, etc. 
 
 (3) Metamorphic minerals, formed, as above explained, from original 
 minerals; e. g., hornblende, albite, biotite, zoisite, garnet, staurolite, 
 andalusite, etc. 
 
 (4) Decomposition minerals ; e. g., chlorite, quartz, carbonates, the 
 hydroxides, etc. 
 
 Such a division, though necessarily not a sharp one, is still not 
 unwarranted and shows how it is possible, with the aid of the micro- 
 scope, not merely to study the composition of a rock in its component 
 minerals, or the conditions under which it was first formed in its 
 
Williams.1 CONTACT AND REGIONAL METAMORRHISM. 3 ? 
 
 structure, but also to trace out life histories. We may discover not 
 only the conditions under which a rock-mass solidified, but we may 
 learn as well something of all the conditions to which it has subse- 
 quently been subjected. 
 
 Metamorphism, or the recrystallization of rocks, whether massive or 
 stratified, igneous or sedimentary, is as varied in its results as the 
 materials acted upon aud the agencies which produce it. How true 
 this is may be seen where the cause of the change is local and well 
 understood, as in the numerous instances of contact-metamorphism 
 which have been studied in detail during the last fifteen years. Here 
 the alteration produced by the same eruptive mass is different in 
 a shale from that in a sandstone, and in each the alteration is quite 
 distinct from that produced in a limestone. If intrusive rocks fall 
 withiu the range of influence, the effects produced in them are again 
 different; while still wider variations are noticeable if the character of 
 the active or metamorphosing rock be changed. This may be seen in 
 the contrast between the effect produced by a mass of granite and a 
 mass of diabase upon the same surrounding rock. Still other differ- 
 ences are traceable to the probable action of vapors, as in the case of 
 a local development of tourmaline or topaz within the limits of a granite 
 contact zone. 
 
 How much greater then might we expect the differences to be which 
 all the complicated and imperfectly understood conditions of regional 
 metaraorphism produce. Many rocks occupying large areas exhibit a 
 character very similar to that of rocks which have been produced by 
 contact-metamorphism, without there being any cause to which the 
 alteration can be so directly attributed. In some schists, like those of 
 the Ardennes Mountains 1 and those of Bergen in Norway , 2 and in 
 many limestones, metamorphic minerals have been extensively devel- 
 oped without the total obliteration of organic remains. In the case 
 of other rocks, of essentially the same character though perhaps more 
 crystalline, the internal evidence or the stratigraphical relations are 
 enough to prove that they are metamorphosed sediments. 
 
 Many of the so called crystalline schists present features of both 
 composition and structure which are strikingly similar to those of 
 rocks of undoubted metamorphic origin, but nevertheless we have at 
 present but few data for constructing a satisfactory explanation of the 
 origin of these enigmatical formations, Theorizing in regard to them 
 has done its best, and has succeeded in introducing only confusion and 
 disagreement. As before remarked, the variety here is far too great to 
 be accounted for by a single hypothesis, however broad. Many agencies 
 have been at work, whose exact nature and importance only the most 
 laborious and patient investigation can show. In working in Archean 
 
 *A. Reward: Lea roclias grenatif&res ct arapliiboliques de la region do Bastogno. Bull. Mua. Roy. 
 Hist. Nat. Belgique, 1882, vol. i, pp. 1-54. 
 
 * H. II. Renach : Silurfoaailer og prcaaedo Konglom crater i Borgonsakifrone, 1882. Germ, tranal. by 
 
 by R. Baldauf. 
 
38 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62 . 
 
 geology the only safe method is to free the mind completely from all 
 traditions and theories — to start with the idea that almost nothing is 
 known with certainty and that everything is to be discovered. The 
 facts must be most critically observed and considered, without too great 
 a tendency to use them at once for the deduction of general principles. 
 Only such conclusions as can not be doubted by any one who will take 
 the pains to examine the facts are of real value to the advance of arch- 
 ean geology; and every careful student in the field must realize how 
 slow and difficult such an advance must be. Detailed analyses of the 
 workings of some well recognized agency, made where the action has 
 been as little as possible disguised and complicated by the action of 
 other agencies, must yield valuable assistance in the penetration of the 
 mysteries which now everywhere surround the prefossiliferous forma- 
 tions of the earth’s crust. Such work has been done in Europe and has 
 been begun in America. The little that has already been accomplished 
 in this manner is full of promise for the future. The most striking ex- 
 ample of work of this kind is perhaps that of Lossen in the Hartz 
 Mountains, and it is with the sincerest appreciation of his method and 
 results that the present studies have been prosecuted. 
 
 If it be granted, as it must be, by every impartial observer that such 
 a thing as regional metamorphism does exist — that certain rocks, wheu 
 they are subjected to enormous strains, and are upheaved, crushed, and 
 crumpled do become more crystalline or have their crystallization al- 
 tered— then we have a well recognized agency whose particular results 
 are worthy of patient and detailed study. What part regional meta- 
 morphism has had in the production of the archean rocks as a whole, 
 future years must show. This question lies wholly without my present 
 purpose; and yet it is hoped that an extended investigation of a par- 
 ticular phase of it may aid in the final solution of the problem. 
 
 The investigation was undertaken with a firm conviction of the pe- 
 culiar advantages offered by eruptive rocks for the accurate tracing of 
 progressive metamorphism, an advantage which Prof. A. K. Lossen 
 seems to have been the first to emphasize, if we may judge from the 
 following extract from one of his papers. He says : 1 
 
 I attribute the extreme value of such metamorphosed eruptive rocks for the general 
 theory of metamorphism to the fact that they are certainly known to have been de- 
 rived from a solid rock of definite mineral aggregation, average chemical composition 
 and structure. In the primary minerals and structures of the igneous rocks we pos- 
 sess a well known quantity, upon which we can base our conclusions — a definite scale 
 according to which the nature and amount of those secondary minerals and 
 structures characterizing the metamorphic rocks can he measured. Frequently 
 the certain, incontestable fact of pseudomorphism proves the secondary alteration of 
 these rocks in a much more general way than even the very exceptionally preserved 
 fossil remains are able to prove the origin of metamorphosed sediments. , 
 
 1 Den hohen Wertk dieser metamorpbiacben Eruptivgesteino fur die Lelire voni Metamorpbismus 
 fand icb darin, dass ein von Ilaus aus festes Gestein vonganz bestimmter Mincralaggregation, chemischer 
 Durchschnittszusammemetzung tend Structur, zuverlassig als ibr Muttergestein angegebeu werden 
 kann. In den priiniiren Mineralicn und primaien Structurpn der Erstarrungsgesteine besitzcn wir eine 
 
WILLIAMS.] 
 
 CHANGES IN ROCK-FORMING MINERALS. 
 
 39 
 
 There is no student of mineralogy who has not been struck with the 
 great similarity which exists in the composition of so many of the 
 rock-forming silicates. 
 
 We have after all a very small number of bases in these silicates and 
 they are often combined in almost the same proportion in minerals 
 which show the greatest disparity of crystal form, physical properties, 
 and mode of occurrence. It seems to be oftentimes more a matter of 
 external condition rather than of chemical composition, which deter- 
 mines what particular mineral is formed ; and the equipoise between 
 the existence of a certain silicate and the external conditions is often 
 so delicate that a mere change in the latter is alone sufficient to de- 
 stroy the mineral as such and to cause it to change to some other mod- 
 ification or compound. The recent discoveries of the alterations which 
 dimorphous bodies, like leucite or tridymite undergo, show how this 
 may be accomplished without chemical change. The breaking up of a 
 mineral into an aggregate of two or more is not less common ; as for 
 example, the passage of piagioclase iuto zoisite and albite (saussiirite), 
 or of spodumene into albite and eucryptite (the /?-spodumene of 
 Brush and Dana .) 1 This subject has lately been elaborated by Prof. 
 J. W. Judd in his presidential address before the Geological Society of 
 London, and in many others of his recent papers . 2 
 
 Bocks whose component minerals are so delicately balanced to accord 
 with the particular set of conditions under which they were formed, 
 must be peculiarly subject to alteration when these conditions are 
 changed j and for this reason the writer lias before insisted that erup- 
 tive rocks must be even more liable to metamorphism than the sedi- 
 ments which contain them . 3 
 
 The advantage, then, of eruptive rocks, especially of basic eruptive 
 rocks, for the study of metamorphic processes is, as Lossen has remarked 
 with so much force, because we have in them a set of minerals and 
 structures which can with certaiuty be referred to eruptive conditions, 
 i. e., conditions of fusion. These, at least for the basic rocks, may be 
 easily reproduced in the laboratory, as has been so successfully done by 
 
 wohlbokannte Grosse, die wir unserem Urtheil zu Grande legen konnen, einon festen Maassstab, ail 
 welchem Art und Grad jener secundaren Mineralien und socundareu Structure!* gemessen werdenkbn- 
 nen welche die Natur des metamorphischen Gesteins melir oder weniger auamacbon. Vielfacb ist es 
 geradezu diesichero, uuanfechtbare Thatsache der Pseudomorphosenbilduug, die in solchen Gestoinon 
 jn viel allgemeinerer Weise bewcisend fur die Umbildung eintritt, ala dio nur unter besonders guns- 
 tigen Umstanden erhalteuon Petrafacton in den metamorpliisirten Sedimenten. Jahrbuck dor kbnig- 
 lichen preussischen geologiscben Landesanstalt u. Bergakademie fiir 1883, Berlin, 1884, p. G20. 
 
 On page 619 ibid., Lossen in a note gives the foll(>wing list of references to his former remarks on this 
 same important topic: Zeitsclirift der deutschon gcologischen Gosollscbaft, vol. 21, p. 298, 1869; vol. 
 24, pp. 706, 707,763, 1872; vol. 27, pp. 451 and 969, 1875; vol. 29, p. 360, 1877; Sitzungsbericlito der Go- 
 sellscliaft naturforschender Freunde in Berlin, Mch., 1878; Jan., 1880, and Nov., 1883; Jahrlmchder 
 kbngl. preuss. geologiscben Landesanstalt fiir 1880, p, 12; fiir 1881, p. 43, and finally in the Erliiute- 
 rungen zur geologiscben Specialkarte von Prcussen und don thiiriugisekon Staaton. Blatter: llarz- 
 gorodo (p. 79) ; Wippra (pp. 27, 43) ; Sohwenda (p. 34). 
 
 1 Am. Jour. Sci., 3d sor., vol. 20, 1880, p. 257, and Zoitschr. Kryst. u. Minoral., vol. 5, p. 192. 
 
 2 Quar. Jonr. Geol. Soc. London, vol. 43, 1887. Proc. pp. 54-82. 
 
 3 Boll. U. S. Geol. Survey, No. 28, p. 9, 10. 
 
40 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62. 
 
 Messrs. Fouque and Michel -L6vy, of Paris. 1 The exact mineral associa- 
 tion and structure of diabase and other basic igneous rocks may be syn- 
 thetically reproduced by simple dry fusion, and there is no indication 
 whatever that they are ever produced in nature by any other means. 
 The finding therefore of such characteristic structure, even where they 
 have been more or less disguised by subsequent changes, at once fur- 
 nishes a definite and certain starting point. We know what the orig 
 inal character of the rocks in question was and the conditions under 
 which it was formed; and the careful minute study of the changes 
 which the original component minerals have undergone, when taken in 
 connection with the external physical conditions to which the rock mass 
 has been subjected, can but yield useful results to geological science. 
 
 HISTORICAL OUTLINE OF STUDIES ON THE METAMORPHISM OF ERUP- 
 TIVE ROCKS. 
 
 Notwithstanding the great importance which has always attached to 
 the idea of metamorphism, it is only within recent years that it seems 
 to have been regarded as applicable to any but sedimentary rocks. 
 With Hutton, who may practically be considered the originator of the 
 idea, and with Lyell, to whom we owe the term which describes it, met- 
 amorphism was the gradual consolidation , by means of the earWs internal 
 heat , of sunJcen and buried strata , whose original parallel structure was 
 not wholly obliterated by the change. So strong has the power of this 
 tradition become, that it is not easy to overcome it even at the present 
 time. Nor after the discovery and satisfactory explanation of second- 
 ary (slaty) cleavage in rock-masses, was the case much better. The 
 distinction between foliation and stratification was accepted as rad- 
 ical, and it was generally conceded that the former was secondarily 
 developed in solid masses as the effect of pressure, and yet we hear of it 
 chiefly in sedimentary rocks — in slates and shales. The eruptive rocks 
 seem to have been regarded as too hard and unchangeable to be affected 
 even by the enormous forces which upheaved a mountain chain. How 
 untrue this is we are daily learning from the study of rocks undoubtedly 
 eruptive, which possess a pronounced schistose structure. 
 
 As we now look back over a century of discussion and investigation 
 of metamorphism, the total neglect of eruptive masses, save as an active 
 agent in the change, seems surprising. Daubree, in his admirable essay 
 on the subject, 2 has much to say of change of structure, and yet he 
 makes no allusion to eruptive rocks as being subjected to it. Delesse, 
 in the second portion of his u Studies of Metamorphism” 3 which treats 
 of regional or normal metamorphism, devotes considerable space to the 
 metamorphism of eruptive rocks, but his conclusions are not such as 
 at the present time deserve attention. He maintains that by some 
 
 1 Synthase ties mindraux et de roches, Paris, 1879. 
 
 3 Etudes et exp6riences synth6tiques sur le m6tamorphi9me, etc., M6ra. presents par savants \ 
 l’AcadSmie des sciences, vol. 17, 1862. Translated in the Smithsonian Annual Report for 1861, pp. 228-304. 
 
 *Etudes sur lemGtamorphisme des roches. Ouvrage couronnG par l’Acad6mie des sciences. Paris, 
 1869. 
 
WILLIAMS.] 
 
 METAMORPHISM OF ERUPTIVE ROCKS. 
 
 41 
 
 vague process of “general metauiorphism ” volcanic rocks are changed 
 to plutonic. Thus a trachyte becomes a granite ; aucl a trap, a diorite. 
 The absence of volcanic rocks in the oldest formations is accounted for 
 by the great length of time during which these have been subjected to 
 metamorphosing agencies. The original plutonic rocks are considered 
 to be capable of little or no change. 
 
 One of the first truly scientific studies of the metamorphism of erup- 
 tive rocks, based purely on careful observation of the facts, was that of 
 Lossen in the Hartz Mountains. Here it was possible to trace the nu- 
 merous diabase dikes and larger areas of more coarsely crystalline gab- 
 bros, along with the schists in which they were inclosed, from their 
 unaltered to their most highly altered form. Ag early as 1872 he wrote 
 as follows: 
 
 I shall begin with igneous rocks which have been altered in situ and with their 
 (final) change into crystalline schists. The fact that massive rocks, which frequently 
 possess a parallel structure as an original feature, may, by metamorpliic processes, 
 be converted into foliated, but not on that account stratified, beds is incontestable. In 
 this manner granular diabase is converted into leuticularly foliated (fiaserig) by the 
 more or less complete passage of the cleavable augite into a scaly aggregate of 
 chloritie minerals. The rock thus assumes a kind of schistose structure, as is often 
 the case in the southwestern Hartz . 1 
 
 The cause of the metamorphism, too, can be seen in some cases to 
 be the eruption of large granite masses ; in others, the orographic forces^ 
 which had crumpled and upheaved the entire district. Upon this subject 
 Lossen says: 
 
 1 have often emphasized the significance of those metamorphic regions in which 
 ernptive rocks— interbedded in the schists and like them jmssively subjected to dis- 
 location and mountain-makiug forces — have undergone about the same substantial 
 and structural alterations as the inclosing schists ; nor is it material whether this re- 
 sult has been accomplished within the coutactTZone of some intrusive granitic mass 
 or by dynamic (dislocation) forces properly so called . 2 
 
 Massive rocks may therefore be passively subjected to the influence 
 of either contact or regional metamorphism. 
 
 Instances of the former seem never to have received their merited 
 share of attention, and yet they have been mentioned in many different 
 regions. Allport described dolerites which had been altered by adja- 
 cent eruptive granites in Cornwall. 3 I 11 France Michel-Levy has found 
 
 ‘lull begiune mit den in situ nnagewandelten Erstarrungsgesteinen und deren TTuawandlung zu 
 krystallinischeu Scbiefern. Die Thatsache, dass durch metamorphische Proces.se inassigo Gesteine, 
 die haufig bereits cine urspriiuglicke plane Parallel structur besitzen, in schioliige, darum aber noch 
 nicht in geschichtete, umgewaudelt werden, ist unbestreitbar. So geben die kbrnigen Diabase dadurch 
 hiiuUg in flaserige Uber, dass das blatterig brechende augitischo Mineral ganz oder theilweiso in oin 
 scbnppiges Aggregat eines chloritischen Minerals urngewandelt wird, wobei das Gestein eino Art 
 echiofrige Structur anuobmen kann, wio dies iin S'udost Harz nicht sclton dor Fall ist. (Zoitschr. 
 Dcutsch. gcol. Gesell., Berlin, vol. 24, p. 763, 1872.) 
 
 2 Merfacb bercits babe ich die Bedeutung solcher metanaorphischer Gebieto hervorgelioben in welchen 
 zwischcn den Schichten eingoscbalteto und nur passiv ana Faltungs- und Gobirgsbildnngsprocosse bo- 
 tboiligto Ei uptivgesteine in anniihernd demsolbon Grade wie die danobon anstehendon Schichtgestoine 
 substantiello nnd strecturello Umwandlungon, sei es in der Contactspkiire der in die Faltuug oingrei- 
 fenden eugranitischen Eruptivnaassen, sei es durch den Dislocationsprocess seb loch thin, orlitten 
 haben. (Jalirb. preuss. gcol. Landesaustalt fiir 1883, p. G19.) 
 
 3 On the metamorphic rocks surrounding the Land’s End mass of granite. Quarterly Journal Geol. 
 Soc., London, vol. 32, 1870, p. 422. 
 
42 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 {BULL. 62. 
 
 similar effects produced in the Cambrian diabases , 1 and Barrois' men- 
 tions diorites ( u diorite modifie”) which have been modified by the same 
 cause . 2 Still more recently Brogger has discovered the same class of 
 phenomena in dikes of augite porphy rite which penetrate the strata of 
 the classic Silurian region near Christiania . 3 
 
 The most exact and satisfactory accounts of such rocks are, however, 
 those given by Lossen of the diabases which fall within the limits of 
 the Bamberg granite contact zone in the Hartz Mountains . 4 The effect 
 of the granite has been to produce alterations in the eruptive diabases 
 quite analogous to those usually brought about by orographic forces. 
 The augite has been changed to uralite, which surrounds the core of 
 the original mineral in a double zone, the inner one being colorless and 
 dotted with magnetite, while the outer one is composed of a more com- 
 pact, green, and pleochroic hornblende . 5 The labradorite of these 
 diabases has been saussuritized; their ilmenite has been changed to 
 sphene (leucoxene) and their pyrite to pyrrhotite. Biotite and garnet 
 have also been occasionally developed. The characteristic diabase 
 structure is recognizable so long as any of the augite or labradorite 
 substance remains. 
 
 If the results described by Lossen are in reality wholly due to the in- 
 fluence of the intrusive granite mass, then we see that the similarity 
 between the effects produced by contact metamorphism and regional 
 metamorphism is just as close in the case of eruptive rocks as it is in that 
 of sedimentary beds. The connection which exists between regionally 
 metamorphosed areas and the disturbances to which such areas have 
 been subjected appears to be a constant one. Indeed, aside from the 
 local influences of intrusive masses, the amount of metamorphism may 
 be said to be in all cases proportional to the pressure or strain to which 
 the rock in question has been subjected. The recent recognition of this 
 fact has brought into favor the term “ dynamic metamorphismj ’ 6 which, 
 in a way, expresses the agency or process to which the change may be 
 attributed. 
 
 Bocks are not metamorphosed by pressure alone, and yet the im- 
 portance of this agency would appear to be greater than that which has 
 commonly been assigned to it. Other factors, especially heat and 
 moisture, have also played an important part in the changes, but their 
 efficacy is in large measure due to the direct results of pressure upon 
 
 1 Sur lea roches eruptives basiqnes Cambriennes du M&connais et du Beaujolais. Bull. Soc. g6ol. 
 France, 3 series, vol. 11, 1883, pp. 273-303. 
 
 2 Lc granite de Eostrenen, ses apophyses et ses contacts. Annales Soc. gdologiquo du Nord, 1884, 
 vol. 12. 
 
 3 Spaltenverwerfungen in der Gegend Langesund-Skien. Nyt Mag. for Xaturvidenskaberne, vol. 
 23, 1884, pp. 253-419. . 
 
 4 Ueber den Kamberg Granit nnd seinen Contact-Hof. Erlauterungen zu Blatt Harzgerode der 
 
 geologischen Specialkarte von Preussen und der thiiringiseben Staaten. Vide also Jahrb. kdn. preuss. 
 geol. Landesanstalt fur 1883, pp. 619-612 ; fur 1884, pp. 56-112, and pp. 525-545. 
 
 6 For an illustration of this structure, see Bull. U. S. Geol. Survey, No. 28, 1886, PI. I. Fig. 2. 
 
 c “Mechanical metamorphism ” of Heim audBaltzer, “ Dislocation-M.” of Lossen, “ Dynamical-M.” 
 of Eosenbusch, “ Stauungs-M.” of Credner, “ Pressure-M.” of Bonney. 
 
WILLIAMS.] 
 
 THREE TYPES OF METAMORPHISM. 
 
 43 
 
 the solid rock-mass. The crushing of rocks along fault or shearing 
 planes allows here of the ready circulation of moisture and of a conse- 
 quent increased distribution of heat. RoeTic are hence most altered 
 along such planes. The almost universal effect of such a crushing is 
 made apparent by a microscopic examination of rocks which have been 
 subjected to enormous pressure. We shall have occasion to cite numer- 
 ous instances of this in the sequel. For the present we will state the 
 three different modes in which an eruptive rock is altered when it 
 undergoes regional or dynamic metamorphism, and mention the work 
 of those who have been particularly successful in illustrating the action 
 of all or any of them. 
 
 The three ways in which a massive crystalline rock may be modified 
 by the action of orographic forces are : 
 
 J. Macro-structural ; i. e., it may have its external structure (mor- 
 phology) changed so as to become schistose or foliated. 
 
 II. Micro- structural ; i. e., it may have its internal or microscopic 
 structure (histology) wholly changed, either with or without an alter- 
 ation of the last-mentioned sort. 
 
 III. Mineralogicai ; i. e., there may be a change in the nature of one 
 or more of the component minerals, either with or without a change in 
 the chemical composition of the rock as a whole. 
 
 Of course, any one of these kinds of change may be produced in a 
 rock-mass alone, or any two, or even all three, may exist simultaneously 
 in any relative degree of intensity. 
 
 Macrostructural Metamorphism. — It had already long been recognized 
 that transversal or slaty cleavage could be produced in sedimentary 
 beds by mechanical force, 1 when A. Heim, in his work on the “ Mech- 
 anism of Mountainmaking,” published in 1878, 2 directed attention to 
 an almost new line of geological work, by showing in a very general 
 way how the orographic forces effect the deformation of rock-masses. 
 He insisted upon three main points: 
 
 (a) That the rocks were solid and rigid when they were acted upon. 
 
 (b) * That by a moderate pressure, they are torn asunder and the thus 
 formed open fissures ( (( klaffende Risse”) are subsequently filled by ma- 
 terial segregated from the rock (“ adern ”). If the mass is plastic rather 
 than brittle, the strain is relieved by numerous slicken-sides ( u Rutsch- 
 flachen”) (“ Umformung mit Bruch”). 
 
 (c) That by the most intense pressure this action becomes infinitely 
 small or molecular, i. e., the form is altered without rupture (“ Umfor- 
 mung ohne Bruch”). 
 
 Heim lays great stress upon the fact, already emphasized by Suess, 3 
 that the massive or crystalline rocks whicli form the center of the Al- 
 
 1 On slaty cleavage awl allied rock-structures with special reference to the mechanical theories of 
 their origin. 13y Alfred Harker. Kept, fifty-fifth meeting Brit. Assoc. Adv. Sci., in 1885, pp. 813-855, 
 
 1886. 
 
 2 Untersuchnngen liber den Mechanismns dor Gebirgsbildung ini Anschluss an die geologische Mono 
 graphic der Todi-Windgallcn-Gruppe. Basle, 1878, Vol. 2. 
 
 * Die Entstehung der Alpen. Wien, 1875. 
 
44 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62. 
 
 pine “massivs” were not themselves in any way instrumental in the 
 elevation of the mountains. He gives an elaborate proof that these 
 were solid long before the elevation ; and were only passively sub- 
 jected to the upheaving force, in the same way as the overlying sedi- 
 ments. Heim does not, however, seem to apply his laws of mechanical 
 deformation to these crystalline rocks, as he might well have done, but 
 regards their schistose or banded structure as probably an original 
 character. 
 
 Other geologists were not long in recognizing the mechanical defor- 
 mation of massive as well as sedimentary rocks. Daubree is struck by 
 the frequent gradual passage of massive rocks into schistose varieties 
 of the same composition. He says that, in spite of his own strong lean- 
 ings toward the u metamorphic theory,” he can not possibly regard 
 such a schistose structure as any sign of original stratification but 
 must consider it as secondarily produced in the eruptive mass by press- 
 ure. He is, however, inclined to believe that this result was attained 
 before the eruptive rock had wholly solidified. 1 H. H. Reusch, from 
 his studies of the rocks near Bergen, in Norway, is also convinced that 
 the frequent banding and gneissic structure in granite is secondary and 
 a product of pressure, like slaty cleavage. Like Daubree, he too thinks 
 that it was accomplished while the rock was still somewhat soft, atthe 
 time of the faulting and dislocation to which the granite owed its own 
 elevation, in a plastic state. 2 This idea that such pressure deformation 
 could only take place in softened or in unsolidified rocks was particu- 
 larly dwelt upon by Carl Friedrich Naumann. How thoroughly the ob- 
 jections to the deformation of rigid rock masses, as far as sedimentary 
 deposits are concerned, are answered by the facts observed by Heim, 
 we have already seen. The assumption of an identical process for the 
 highly crystalline massive rocks seems, at first, to present great dif- 
 ficulties, but observations in all parts- of the world are daily proving 
 its necessity. 
 
 In 1879, Rothpletz 3 showed how the actinolite, or so-called green- 
 schists near Hainichen, in Saxony, had been brecciated by pressure and 
 the fragments shoved along more or less upon each other, so as often 
 to produce an imperfect schistose structure. This, which has a close 
 analogy to certain macros tructural modifications of the Lake Superior 
 greenstones to be described in subsequent pages, allowed, as Rothpletz 
 remarked, a much increased chemical action, which tended to alter the 
 character of the rock. A. Baltzer, in his monograph on the Finster- 
 aarhorn, 4 published in 1880. expresses himself as decidedly in favor of 
 a mechanical metamorphism of the interior crystalline rocks. He says 
 on page 244 of his work : 
 
 1 iStudes synthbtiques de g6ologie exp6rimeutelle. Paris, 1879, p. 432. 
 
 2 Die fossilien fiihrenden krystallinischen Schiefer von Bergen in Norwegeu. Deutsche Aufgabe von 
 It. Baldauf, 1883, pp. 129, 130. 
 
 3 Uel>er mechanisclien Gesteinsumwandlungeu bei Hainichen in Sachsen. II. Die Breccienbild- 
 nng des Aktinolitlischiefers von Hainichen. Zeitschr. Dentsch. geol. Gesell, 1879, Vol. 31, p. 374. 
 
 4 Die mechanisclie Contact von Gneiss und Kalk iui Berner Oberland. Beitrage zur geologischen 
 Karte der Schweiz. XX. Lieferung. Bern, 1880. 
 
WILLIAMS.] 
 
 LEHMANN ON DYNAMIC METAMORPHISM. 
 
 45 
 
 I base my assumption that the parallelism of the mica-scales in abnormally strati- 
 fied gneiss is conditioned by pressure, upon this transverse foliation. Just as slaty- 
 cleavage is generated in the younger sedimentary rocks by pressure and mechanical 
 deformation, so is it also in the crystalline schists. This may be proved in the case 
 of the last named rocks, if other evidence is lacking, by its parallelism with the un- 
 doubted cleavage in contiguous sediments . 1 
 
 Similar ideas have been more or less clearly expressed by Kjerulf, Brog- 
 ger, Stapff, and other geologists,but one of the most important contribu- 
 tions to our knowledge of this, as well as of other phases of mechani- 
 cal metamorphism, was made in 1884 by Prof. Johannes Lehmann in his 
 work on the origin of the crystalline schists. 2 That author has col- 
 lected an immense number of observations from Saxony, Bavaria, and 
 Bohemia — especially in the “ Granulite 79 district of the first named 
 country, upon the detailed study of which he has spent many years. 
 From these observations Lehmann reaches certain general conclusions 
 of importance with reference to the mechanical metamorphism of solid 
 massive rocks. These are stated in chapters 16 and 17 of his ‘work. 
 He regards gneiss as simply a structure form of granular feldspathic 
 rocks, and according to the composition of these there may occur gran- 
 itic gneiss, syenitic gneiss, dioritic gneiss, gabbro gneiss, etc. He thinks 
 that the essential parallel structure of gneiss may be, but very rarely 
 is, original. He finds no indication that any true gneisses were once 
 sedimentary deposits, but he considers them all as igneous rocks 
 (“Erstarrungsgesteine”), which, as a general thing, have acquired their 
 present structure by stretching (“ Streckung”) in a solid state. More- 
 over, gneiss exhibits only the first stage of such a mechanical meta- 
 morphism. If the action of this process is more intense, finer grained 
 and more evenly banded rocks result, which the author designates as 
 granulite and felsite schist. According to Lehmann, therefore, all the 
 massive crystalline rocks are subject to alterations in their structure 
 through great pressure or tension. They become banded or schistose in 
 proportion to the intensity of this action. 
 
 The observations of many workers in various regions since the publi- 
 cation of Lehmann’s conclusions have tended to substantiate them. 
 Mr. Hatch 3 has shown the secondary development of a schistose struct- 
 ure in the gabbros of the Tyrol, and the same thing has been done for 
 the gabbros near Baltimore, Maryland. 4 Besults very closely resem- 
 bling those of Lehmann have recently been secured by Mr. J. J. H. 
 Teall in the gabbro region of the Lizard, Cornwall, England. 5 This 
 
 1 Auf diese transversale Scliieferung griinde ich die Annalime dass dor Paralloliruus der Gliminor- 
 blatrchen ira anonnal gelagerten Gneiss ebenfalls von Druckschieferung herriihrt. Wio in don jiing- 
 ern Sediraentgesteincn durch Druck und niechanisclie Umformungsprozesso transvei salo Sckieferurig 
 entstand, bo anch in den krystallinisclien Schieferu. Bei letzteren kann sie, in Ermangelung andorer 
 Anhaltspuukto, durch den Parallelismus mit einor uuzweifelliaften Schieforuugsrichtung in don au- 
 grenzenden Sediruenten nachgewiesou werdon. 
 
 ’Untersuchnngen iiber die Entstobung der altkrystallinischon Schioforgestoine, etc., with Atlas of 
 photographs. 4°. Bonn, 1884. 
 
 *T«ohermak’s mineral, ti. petrog. Mittheil., vol. 7 (1885), p. 75. 
 
 4 Bull. U. S. Geol. Survey, No. 28. 
 
 •Geol. Mag., London, November, 1886. 
 
46 GREENSTONE # SCHIST AREAS OF MICHIGAN. [bull. 62. 
 
 investigator derives proof that the alteration ip structure was accom- 
 plished after complete solidification from the relation of the rock to 
 fault-planes. He says: 
 
 A rock must necessarily be solid before it can be faulted. Now, we find at Pen 
 Voose near Landewednack, that massive gabbro passes over into gabbro schist at a 
 fault-plane, and that the foliation in the gabbro is such as would be produced by a 
 shearing motion parallel with the fault-plane. Taking all the facts into considera- 
 tion, we appear to be justified in concluding that the foliation in the Lizard gabbros 
 is the result of pressure or regional metamorphism. 
 
 O. Schmidt has also recently given us the results of his studies of 
 certain eruptive porphyries in the central Alps, especially in the Wind- 
 gallen group, the district particularly studied by Heim. 1 These, like 
 the surrounding sediments, have been subjected to euormous pressure 
 and strains and thereby have had developed in them a pronounced 
 schistose structure, becoming in some instances veritable felsite schists. 
 Still more recently H. H. Reusch has communicated his observations 
 in the regionally metamorphosed district of Hardangerfjmxl, on the 
 west coast or Norway. 2 Here he finds dikes of all sorts of eruptive 
 rocks, both acid and basic, all rendered secondarily schistose parallel 
 to the planes of the inclosing schists, without reference to the direction 
 of the dikes themselves. This, therefore, can not possibly be due to 
 either flow or cooling, but must be the result of pressure. Oh. E. 
 Weiss observed the same thing in the quartz porphyry dikes of Thai, in 
 Thuringia. 3 
 
 Prof. T. G. Bonney, in his annual presidential address to the Geo- 
 logical Society of London (February, 1886), deals with the subject of 
 metamorphism in general, and has much to say about the structural 
 changes induced in hoiocrystalliue massive rocks by pressure 4 . He 
 distinguises between u stratification- foliation” and u clear age-foliation fi 
 the latter being always secondarily produced by pressure. 5 This same 
 cause also in some cases may produce a false bedding parallel to the 
 cleavage-foliation, almost exactly similar to the bedding of sedimentary 
 rocks, although of a totally different origin, and to this he applies the 
 name u pseudostromatism.” 6 
 
 Microstructural metamorphism. — The statement of Heim that under 
 sufficient pressure rock-masses became plastic, i. e., that they could be 
 bent and crumpled by a true molecular movement within the mass, with- 
 out rupture, seems to have been based entirely on a macroscopical study 
 of exposures and specimens. Rocks, and even their constituent miner- 
 als, certainly do appear to the unaided eye to be stretched and contorted 
 without any break in their continuity. Whether, however, this effect 
 is accomplished by a truly molecular movement, as in a viscous body, 
 
 1 Xeues Jahrbucb flir Miueralogie, etc., Beilageband 4, p. 388, 1886. 
 
 2 Ibid., Beilageband 5, p. 56, 1887. 
 
 3 Zeitechr. Deutscli. geol. Gesell., vol. 36, 1884, p. 858. 
 
 4 Quar. Jour. Geol. Soc. London, vo). 42, 1886, Proc., p. 95. 
 
 6 Ibid., p. 64. 
 
 6 Ibid., p. 65. 
 
williams.] DEFORMATION OF ROCKS WITHOUT RUPTURE. 
 
 47 
 
 or by a breaking or crushing of the component crystals with a move- 
 ment in the mass before it is recemented, is something that can not 
 be well decided by the unaided eye. Such authorities as Giimbel 1 and 
 Pfaff 2 at once took exception to the conclusions of Heim, and stated it 
 as their conviction that, strictly speaking, there was no such thing as 
 the deformation of rocks without rupture. Baltzer 3 could not decide 
 between the conflicting views, but thought there was probably truth 
 in each. The microscopical study of such bent and contorted rocks 
 seems to show that the explanation of Giimbel is generally the true one. 
 This was emphasized by J. Lehmann . 4 He calls attention to the fact 
 that the conception of plasticity is not a simple one. We speak both 
 of wax and of wet clay as “ plastic,” and yet the movement of the 
 homogeneous body is different from that in the heterogeneous substance. 
 In each the process of the deformation escapes the eye and the results 
 appear the same; but in reality the first is molecular, the second 
 caused by the slipping of the component particles (kaolin scales) over 
 each other. In rocks the “plasticity” is of the second kind. Lehmann 5 
 says: 
 
 When rock-deformation has been accomplished by a breaking and sliding of the 
 individual constituents upon each other, I think that I am still justified in calling it 
 a deformation without rupture, provided the continuity of the rock-mass itself has 
 been preserved and no fissures have been formed. * * * I recognize only that as 
 
 rock-deformation with rupture when fissures, even though microscopic, traverse the 
 rock independent of the individual constituents . 6 
 
 Again he says : 7 
 
 A plastic molding of the separate constituents, as is assumed by Heim, I have 
 nowhere been able to discover. On the other hand, the maximum of resistance 
 which a crystalline grain can offer to bending or crushing is very soon reached, and 
 then ensues a pulverizing or chemical solution . 8 
 
 Lehmann also particularly emphasizes the importance of the very 
 much increased chemical action which such a crushing of the rock 
 components permits. This had heretofore been almost overlooked by 
 all the students of dynamic or mechanical metamorphism except Lossen. 
 The ease with which a ready circulation and changed physical condi- 
 tion allow the destruction of certain chemical compounds, and the iin- 
 
 1 Das Verhalten tier Schichtgesteine in gebogenen Lagen. Sitzungsberichto dor bon. bayriscben 
 Akademie. Math.-phys. Claase, vol. 4, p. 596, 1880 {reviewed by Rosenbuseh in the Neues Jahrbuck 
 fur Mineral.. 1882, vol. 1, Referate, p. 221). 
 
 2 Der Mechanismus der Gebirgsbilduug. neidelberg, 1880, p. 140. 
 
 3 Die mechaaiache Contact von Gneiss uud Kalk irn Berner Oborland, Bern, 1880, p. 240. 
 
 4 “ Untcrsuchungen iiber die Entstehung der altkryatalliniscLien Scbiefergeateine, etc..” Chap. xvr. 
 
 5 Ibid., p. 245. 
 
 °Ich glaubo aogar mit Recht eino Gostoinsformung, bei welcbcr nur die einzelnen Gemongtheile 
 zcrapalten und aich an einander verschiebon, ala eino bruchloso bezoickneu zu kduen, weuu daa 
 Geatein seiner. Zusammenhalt bewahrt hat uiul koine das Gestoin durchsttzenden Risso vorhanden 
 sind. * * * Eino Gesteinsformung mit Brucli erkeune ich erst d&tm an, wenn Risso, und indgen os 
 auch mikroskopischesein, unbekummert uni die Einzelgeincngthoilodaa Gcatoinagowebodurchsetzen. 
 
 7 Ibid., p. 240. 
 
 ®Einc plastiache Formungder Einzelgomongthoilo, wie aio Heim annohmon zu miiasen glaubt, habo 
 icli niemals gefunden ; vielmehr erreicbt die Biegung oder Zusamnu ndi uckung cinoa Krystallkorns 
 Behr bald daa Maximum uud erfolgt daun eino Zertrurnmorung bozichungaweiso auch eiue ckemiscko 
 
 Aufliisung. 
 
48 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 mediate formation of others out of their elements, is calculated to pre- 
 serve the continuity of tlie rock-mass in spite of extensive stretching 
 or compression. 
 
 Such chemical changes will form the subject of the following section. 
 Here we are concerned only with the mechanical deformation of the 
 elementary minerals. 
 
 The effects of pressure will naturally be first noticeable upon an 
 elastic mineral like mica. A bending of the lamellae is well known to 
 result frequently from even the slight movement of an eruptive magma 
 before its complete solidification. Wherever, therefore, so sensitive a 
 mineral presents no pressure effects when more brittle substances show 
 them, it is fair to assume That the mica has been secondarily developed 
 during the action of the pressure. 
 
 Harder minerals, like augite or feldspar, under the first action of 
 strain, before their cohesion is overcome, appear to have twinning 
 lamellae developed in them parallel to certain planes — and most abun- 
 dantly where the strain is the most intense. To this succeeds a crack- 
 ing of the crystal, with often a considerable separation of the parts and 
 a filling of the interstices by newly depositech substance . 1 A still more 
 intense pressure accompanied by a shearing stress seems to produce a 
 regular granulation of the larger crystals, so that around their edge 
 they pass into a mosaic-like aggregate of fine interlocking grains. 
 This process in the case of augite, as in the Saxon “ Fiaser-Gabbros,” 
 is attended by uralitization, or the production of secondary ampliibole. 
 The resulting structure, in which larger grains are separated by a 
 finer mosaic, has been called by Tornebohm, who observed it in cer- 
 tain Swedish granites, “mortar-structure” (“Moitel Structur ”). 2 This 
 granulation, with increasing strain, may exteud farther and farther 
 inward until finally the entire crystal is replaced by a fine mosaic of 
 interlocking grains. When produced under the influence of sufficient 
 pressure, it may, of course, give rise to a pronounced banded or schis- 
 tose structure. 
 
 The action of strain upon the hardest and most brittle of the rock- 
 forming minerals — quartz — seems to result in cracking and breaking, 
 rather than in bending it. Crystals which appear in hand-specimens 
 to be stretched out into lenses, are shown by the microscope to be com- 
 posed of smaller grains, more or less difierent in their optical orienta- 
 tion. Of this mineral Lehmann says : 3 
 
 The phenomena which the quartz of stretched rocks exhibit manifest themselves 
 under the polarizations microscope in the unequal extinction of dilfereut fields, and 
 
 1 See Lehmann's Atlas, PI. 6, Figs. 3, 6, and PI. 21, Figs. 3, 6. 
 
 2 Nagra ord om granit och gneis. Geol. Foreningens Stockholm Forhandl.,vol. 5, pp. 233-248, 1880- 
 81 (review in the Roues Jahrbuch fur Mineral., 1881, vol. 2, Referate, p. 50). Tornebohm, in this 
 paper, considers this as an original structure. Kjerulf designates all such dynamic changes as are 
 manifested in a movement among the fragments of broken crystals as “ Kataklas-structur." He dis- 
 tinguishes three grades of intensity. See Grundfjeldsprofilet ved Mj^scns sydendo. Nyfc Mag. for 
 Naturvidenskaberne, vol. 29, p. 215, 1885 (review Neues Jahrbuch fur Mineral., 1886, vol. 2, Refer- 
 ate, p. 244). See also Rosenbusch : Mikros. Physiog., vol. 2, 2d cd., p. 42, 1887. 
 
 *TJntersuchungen fiber dio Entsteliung der altkrystalliuischen Schiefergesteine, etc., p. 250, 
 
WILLIAMS.] 
 
 DEFORMATION OF QUARTZ. 
 
 49 
 
 then in a somewhat more exact separation of these fields. We imagine that we can 
 detect sharp boundary lines without being able to certainly prove their existence 
 (and in reality they are due merely to tension). Finally, however, the individual 
 grain does really break up into separate interlocking parts, which at first are but 
 slightly chauged in their orientation. Nevertheless, toward the edge and in the 
 more compressed portions these parts are quite irregularly orientated and participate 
 in the composition of the ground mass. True bending of quartz is unknown to me. 
 It is shattered very easily, and, as it seems, is as readily subject to chemical solution . 1 
 
 Prof. Oh. E. Weiss, of Berlin, describes remarkably deformed 
 quartzes in the schistose porphyries occurring in the almost horizontal 
 mica schist near Thai in Thuringia. 2 This rock forms dikes which cut 
 across the bedding of the schist and send apophyses in a horizontal 
 direction between its layers. The schistose structure of the porphyry 
 was formerly considered to be a flow structure, but Weiss has shown 
 that this can not possibly be, as it runs in every case parallel to the 
 bedding of the mica-schist without reference to whether this is parallel or 
 perpendicular to the walls of the dike . The porphyritic quartz crystals in 
 these rocks are drawn out into long, pear-shaped or tadpole-like (“kaul- 
 quappenahulich”) forms, which follow the direction of the schistose 
 structure. This is accomplished sometimes with, sometimes without, a 
 rupture of the quartz substance, and produces what Lossen calls tailed- 
 quartzes. (“ Schwanzchen-quarz.”) 3 
 
 It is remarkable that the porphyritic feldspar crystals of these 
 rocks have suffered far less deformation than the much harder quartzes, 
 an observation which, as we shall see, is abundantly substantiated iu 
 the schistose porphyries of the Lake Superior region. The phenomena 
 exhibited by the Thuringian rocks, although left without explanation 
 by Weiss, are referred without hesitation by Rosenbusch to the effects 
 of dynamic metamorphism. 4 
 
 Rosenbusch also remarks that, as a rule, the peripheral granulation, 
 (“randliche Kataklase”), characteristic of the coarse-grained, granitic 
 rocks, is wanting in the porphyries. This he attributes to the structure, 
 for in the granular rocks under great pressure the grains rub against 
 each other, while in porphyritic rocks the larger crystals are imbedded 
 in a homogeneous matrix, so that they are either only optically dis- 
 turbed or completely pulverized. 5 
 
 1 Die Erscbeinungen, wolche der Quarz gestreckter Gesteine zeigt, bekundeu sich unter dem Po- 
 larisationsmikroskop in einem ungleiohen Dunkelwerden verscbiedenor Felder, dann in oiner schar- 
 feren Abgrenzuug derselben ; man glaubt Begrenzungslinien zu sehen, obne dass solche thatsacli- 
 lich nachzuweisen warcn — aie beruhen wobl nur auf Spannungen— endlieli zerfallt das einlioitliclio 
 Korn aber wirklich in einzelne, zackig begrenzte Tlieile, dio zunachst nur wonig aus ihrer Lago 
 gedrelit erscheinen ; gegen den Rand des Korns und in starker gepressten Tlieilen jedoch wirr durch- 
 einanderliegen und an der Zusammensotzuugder feinkdrnigeu Grundraassosich bethciligen. Eigent- 
 liche Biegungen von Quarzon sind mir nicht bekannt ; er zerstiickt und zerfallt sehr leiclit und 
 erliegt wie es scheint ebonso leicht einer chomischon Aufldsung. 
 
 2 Jahrbuch preuas. geol. Landesanstalt fur 1883, pp. 213-237, Berlin, 1884; and Zoitsch. Deutsch. 
 geol. Gesell., vol. 36, 1884, p. 858. Cf. J. G. Bornemann: Jahrbuch prouss. geol. Landesanstalt far 
 1883, pp. 383-409, Berlin, 1884. 
 
 * Zeitscli. Deutscb. geol. Gesell., vol. 34, 1882, p. C78. 
 
 4 Die massigon Gesteine, 2d ed., 1886, p. 214. 
 
 6 Ibid., p. 413. 
 
 Bull. 62 4 
 
50 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 (BULL. 62. 
 
 Dr. C.Chelius describes compressed and schistose granite porphyries 
 from the northern portion of the Oden wald (Hesse-Darmstadt). In these 
 the ground-mass is quite fine-grained, but where small areas of it have 
 been protected, as it were, by large porphyritic crystals it has nearly 
 ticice as coarse a grain, 1 
 
 It would appear to be quite generally the case that porphyritic 
 massive rocks, when subjected to great pressure, develop the so-called 
 u Augen structure.” The larger crystals are only partially pulverized, 
 and have on either side of them, in the direction of the schistose struct- 
 ure, a mosaic of their own debris, arranged like the “ crag-and-tail ” of 
 a glaciated ledge. This has been observed and admirably described by 
 Lehmann 2 in the Saxon granulites, by Teall 3 in the gabbros of the 
 Lizard district, Cornwall, and by JBonney. 4 
 
 Miner alogical metamorphism. — This is undoubtedly the most impor- 
 tant phase of metamorphism in eruptive as well as in sedimentary rock 
 masses. It always accompanies such mechanical deformation — whether 
 macroscopical or microscopical — as has been already described ; but, 
 while such dynamic processes may greatly facilitate chemical action or 
 molecular rearrangement, they are by no means always necessary to 
 bring them about. The adjustment between the chemical combina- 
 tions and external conditions is so delicate in the inorganic world as 
 to make the difference, in this respect, between minerals and living or- 
 ganisms seem rather one of degree than of kind. This point has been 
 elaborated by Professor Judd in his recent annual address before the 
 Geological Society of London (February 18, 1887). 5 Wadsworth 6 has 
 also insisted that the, changes in the mineral world are due to the pas- 
 sages from states of less stable to those of more stable equilibrium ; 
 but, as Judd justly remarks, the cycle of changes may be infinite because 
 the stability of a compound depends upon its surrounding conditions. 
 With a change of these, a state which was once stable becomes unstable. 
 No student of mineralogy can fail to appreciate the extreme delicacy 
 of the equipoise. Any one who has produced artificial twinuing-lamellae 
 in feldspar or calcite, or watched sulphur or boracite or tridymite or 
 leucite pass from one modification into another, must acknowledge the 
 importance of paramorphism in the formation of rocks. But changes 
 of minerals accompanied by changes in the chemical nature of the com- 
 pound are still more common. These may consist (1) in the breaking up 
 of one molecule into two or more, with but little replacement of sub- 
 stance, as in the formation of saussurite from labradorite, or of spodu- 
 mene (aibite + eucryptite) from spodumene; or (2) in a reaction which 
 takes place between two contiguous minerals, each supplying a part of 
 
 1 Notizblatt des Vereins fur Erdkundo z u Darmstadt, 4. Folge, Heft 5, 1885, p. 20. 
 
 2 TTntersuchungen iiber die Eutstehung der altkrystallinischen Schiefergesteine, etc. Bonn, 1884. 
 
 3 Geol. Mag., London, Nov., 1886. 
 
 4 Presidential address to the Geological Society, Feb., 1886., Quart. Jour. Geol. Soc. London, vol. 42, 
 
 Proc., p. 96. 
 
 6 See also the writer, Top. Sci. Monthly, Sept., 1889. 
 
 6 Nature, March 3, 18S7, p. 417. 
 
WILLIAMS.] 
 
 MINERALOGICAL METAMORPHISM. 
 
 51 
 
 the substance necessary to form a new compound of intermediate com- 
 position, more stable for the then existing conditions than either. Such 
 a case is the formation of a hornblende zone between crystals of olivine 
 or hypersthene and plagioclase, or of the so-called u kelyphite” zone 
 between pyrope and serpentine; (3) in more complicated and less 
 easily understood chemical reactions, like the formation of garnet or 
 mica from materials which have been brought together from a distance 
 and under circumstances of which it is at present impossible to state 
 anything with certainty. 
 
 All such changes involving an actual change in the chemical com- 
 - position are best designated in contrast to those produced by para- 
 morphism, as metasomatic. 1 
 
 Of course all of these metamorphic changes of a mineralogical char- 
 acter — whether paramorphic or metasomatic — may go on in all conceiva- 
 ble proportions in a rock mass at the same time. They are often 
 accompanied by changes in the original structure of the rock, but not 
 of necessity, although such changes of structure can not be accom- 
 plished without chemical alteration. 
 
 Chemical changes in minerals and rocks have occupied the attention 
 of mineralogists and chemists from the beginning of the century, and 
 yet it is almost exclusively in sedimentary rocks that such studies have 
 been carried on. Only within recent years have the mineralogical met- 
 amorphoses which take place in eruptive rocks commenced to receive 
 their proper share of consideration. Lossen, Tornebohm, and J. Leh- 
 mann. were the first in Europe to recognize the importance of such in- 
 vestigations; while it will ever remain one of the most signal services 
 which Dr. Wadsworth has rendered to petrography that he was the 
 first in America to fully grasp their significance and to emphasize it. 
 
 It would be quite beyond the purpose of the present paper, even if 
 it were possible, to give a complete summary of all that has been done 
 on the subject of chemical changes in eruptive rocks. In this place the 
 attempt will be made only to trace out historically some of the more 
 important alterations which have a direct bearing upon the rocks form- 
 ing the subject of this investigation. Important and wide-spread phases 
 of the metamorphism of eruptive rocks — such, for instance, as serpen- 
 tinization — which are not exemplified within the area studied will not 
 be here considered. On the other hand, minor details or local modifi- 
 cations of well known and universally recognized processes will be elab- 
 orated in the course of the special petrographical descriptions (Chap- 
 ters II-V) and summarized in Chapter VI. 
 
 The points which will be historically considered in this chapter are 
 t lie following : 
 
 ( l.)Uraliiization , or the secondary origin of hornblende, both fibrous 
 and compact, from pyroxene. 
 
 1 This term is preferred to mcthylosig of Kin" and Rownoy (“An old chapter of the geological record 
 with a new interpretation;" London, 1881), and Bonney (Quart. Jour. Gool. Soc., London, vol. 42, 
 1886 , Proc., p. 59), and to metachemic of Dana (Am. Jour. Sci., 1886, 3d sories, vol. 32, p. 70), because it 
 is at present so much rnoro widely used and honco so much moro intelligiblo. 
 
52 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 (2.) Chloritization. 
 
 (3.) Fpidotization. 
 
 (4.) Formation of the viridite (chlorite) epidote aggregate. 
 
 (5.) Saussuritization. 
 
 (0.) Formation of the albite mosaic . 
 
 (7.) Sericitization. 
 
 (8.) Alterations of titanic-iron. 
 
 Uralitization. — Ever since the classic record of observations made by 
 Gustav Rose in the Ural Mountains in 1830, 1 the fact has remained un- 
 disputed that pyroxene sometimes changes to an aggregate of amplii- 
 bole needles which often preserve by their arrangement the original 
 augitic form. It was not long before other similar occurrences were 
 discovered, notably in Scandinavia and the Tyrol. Still, these localities 
 were regarded as exceptional, and it was impossible that the full geo- 
 logical importance of Rose’s uralite should be appreciated without the 
 aid of the microscope. With the help of this instrument it was soon 
 discovered that the smaragdite of the saussurite gabbros or euphotides 
 was a secondary hornblende which had originated from the diallage. 
 As the number of observers and observations increased, instances of 
 the undoubted passage of every sort of pyroxene into a fibrous arnphi- 
 bole grew constantly more and more abundant. It would be useless 
 to attempt "to trace out these discoveries in detail. It is enough merely 
 to mention the names of Rose, Vom Rath, Fischer, Hagge, Zirkel, Von 
 Lasaulx, Rosenbusch, Tornebohm, Svedmark, Sjogren, Becke, Kioos, 
 Micliel-L6vy, Allport, Phillips, Teall and Hatch, in Europe, and of 
 Hawes in this country, to recall the accuracy and value of the facts re- 
 corded, while among the first to see further than mere facts and to grasp 
 the full geological significance of this wide-spread change may be placed 
 Lossen, Lehmann, Reusch, Wadsworth and Irving. 
 
 The alteration of pyroxene to hornblende is almost universally alluded 
 to as paramorphism, and such, indeed, it may be in some instances. 
 Still, many investigations go to prove that it is very often, perhaps al- 
 ways, accomplished by chemical change. The original uralite of Rose 
 was too soft and hydrous to be compared with hornblende. The studies 
 of Forschhammer, Rose, 2 and Svedmark 3 showed that when augite 
 changed to fibrous hornblende, magnetite and often calcite was sepa- 
 rated out between the needles. A recent opinion by Rosenbusch on 
 this point is as follows : 
 
 This uralitization can hardly he regarded as a simple act of molecular rearrange- 
 ment; we should rather expect that apart of the lime contained in the augite would 
 pass into other combinations, and, in fact, epidote is an almost constant companion 
 of uralite . 4 
 
 1 Poggendorff Aniialen, vol. 22, 1831; vol. 31, 1834, p. G17; al&o Iieise nacb dein Oral, vol. 2, p. 342. 
 
 2 Zeit8clir. Deutscb. gool. Gesell. Berlin, vol. 16, 1864, p. 6. 
 
 3 Neues Jabvbucb fur Mineral., 1877, p. 99; Mikros. Pliysiog., vol. 2, 2d ed., p. 185; vol. 1, p. 472. 
 
 4 Diese Uralitisirung kann nicht wobl oin einfacber Act raolecularer Uralagerung sein, es ist viel 
 mebr zu erwarten, dass ein Tk6il ties Kalkgebalts des Augits in andero Verbindungen iibergeho und 
 tbatsachlicb ist Epidot ein nabezu constanter Begleiter des Uralits. 
 
WILLIAMS.] 
 
 UEALITIZATION 
 
 58 
 
 Dr. B. Harrington, of Montreal, has carefully analyzed three stages 
 of alteration between pyroxene aud a secondary fibrous hornblende 
 resulting from it, and has found that during the change there has been 
 a great loss of lime and a gain of magnesia, silica, and the alkalies. 1 
 The specimen investigated was one of the excellent examples of uralite 
 from the apatite mines near Ottawa, Canada, similar to those named 
 by Thomson “ Rapliilite.” 2 
 
 Mr. J. J. H. Teall has also recently discussed this point in connec- 
 tion with his studies of the alteration of the Scourie dike, 3 and is of the 
 opinion that the oxidation of iron from the ferrous to the ferric state is 
 incident to the change of augite to hornblende. 
 
 While the alteration of almost any pyroxene into fibrous hornblende 
 has now become a universally recognized fact, the possibility of the 
 chaugeof this mineral directly into compact hornblende is by no means 
 so generally admitted. So admirable an observer as J. H. Kloos has 
 recently based his distinction between primary and secondary aiuphi- 
 bole in the Black Forest gabbros entirely upon their compact or thin 
 fibrous character. 4 Still, the work of many investigators shows that 
 this is by no means a reliable criterion in all cases. 
 
 Svedmark found in 187I) that the pyroxene of the Yaksala porphyry 
 passed into an aggregate of stout, compact amphibole needles. 5 In 
 1877 Streng described compact brown hornblende in the Minnesota 
 gabbros, which he considered to have originated from the diallage; 6 
 and in 1878 Dr. George W. Hawes described and figured similar occur- 
 rences in certain New Hampshire rocks. 7 In 1880 appeared accounts 
 by Irving, and in 1882 by both Irving aud Yan Hise, of compact brown 
 hornblende originating from diallage. 8 In 1880 C. von John described 
 the alteration of diallage to compact brown hordblende in the olivine 
 gabbro of Bosnia. 9 In 1883 Hj. Sjogren regarded the irregular spots 
 of compact brown hornblende which occur in and around the pyroxene 
 of the wernerite or dipyre-diorite of Bamle in Norway as produced by 
 a molecular rearrangement of the pyroxene substance. 10 In 1884 similar 
 observations were made by myself in certain pyroxenites of the “ Oort- 
 landt Series,” occurring at Montrose Point on the Hudson River; also 
 in the so called u black granite” (gabbro) from Addison, Me., and in 
 rocks from the apatite regions of Canada. 11 In the same year (1884) 
 
 ‘Geol. Survey, Canada. Keport of progress for 1878-79. Appendix G, p. 23. 
 
 2 Outlines of Mineralogy, Geology, etc., London, 1836, vol.,1, p. 153. 
 
 8 Quart. Jour. Geol. Soe. London, vol. 41, 1885, p. 137. 
 
 4 Ncuc8 Jahrhncli fur Mineral., Beilage-Band 3, 1884, pp. 32, 33. 
 
 6 Geol. Fbrcningens Stockholm Fdrhandl., 1876, pp. 151-164 ; Neues Jalirbuch fiir Mineral., 1877, p. 99. 
 
 6 Ncucs Jahrbuch fiir Mineral., 1877, pp. 133, 240; Am. Jour. Sci., Dec., 1884, p. 4C4. 
 
 7 The Geology of New Hampshire, vol. 3, 1878, j>art iv, Mineralogy and Lithology, pp. 57, 206, pi. vii, 
 
 fig 1. 
 
 8 Gool. Wisconsin, vol. 3, (1880) p. 170; vol, 4, (1882) p. 662. See also Geol. Wisconsin, vol. 1, 1883, p. 
 321, and Am. Jour. Sci., 3d series, vol. 26. p. 29, 1883. 
 
 •Grundlinien der Geologic von Bosnieu- Herzegovina* Wien, 1880. (Cf. Neues Jalirbuch fiir Mineral., 
 1881, vol. 2. Ileferate, p. 353.) 
 
 10 Geol. Fdreniugens Stockholm FfSrhnndl., vol. 6, p. 447, 1883. (Cf. Neuos Jahrbuch fiir Mineral. 
 1884, vol. 1. Keferate, p. 81.) 
 
 11 Am. Jour. Sci., 3d series, vol. 28, Oct., 1884, p. 261. 
 
54 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 A. Sckenck quotes in his Inaugural Dissertation a statement made by 
 von Lasaulx in 1878, that pyroxene passes first into fibrous and subse- 
 quently into compact brown hornblende. 1 Sckenck himself observed in 
 the Rimberg diabase from the upper Ruhr Valley that the reverse of 
 this was true, i. e., that the pyroxene passed first into compact brown, 
 and this subsequently into fibrous green hornblende. 2 
 
 The secondary hornblende, so well described and figured by Teall in 
 the Scourie dike, is decidedly compact in its nature, 3 nor is that derived 
 from the paramorphism of the diallage in the Saxon u flaser-gabbros,” 
 according to the observations of J. Lehmann, less compact. 4 Such 
 eminent authorities as Lossen 5 and Rosenbusch 6 also allow that there is 
 no doubt that compact basaltic hornblende occasionally results through 
 the direct paramorphism of diallage, or even orthorhomi ic pyroxene. 
 The chemical composition of the original mineral undoubtedly largely 
 conditions the nature of the resultant product. This is shown by the 
 observations of vou John in the Flysch-gabbros of Bosnia, where brown 
 hornblende resulted from dark and green hornblende from pale diallage. 7 
 
 These facts are dwelt upon here somewhat in detail because, as will 
 been seen in the sequel, they have possibly an important bearing on a 
 large part of the Menominee River greenstones. 
 
 It is not intended, of course, to imply by the above statements that 
 true parallel growths of primary augite and primary brown hornblende 
 may not occur, as held by both Lossen and Rosenbusch (loo. cit.). 
 Such parallel growths would have the closest possible resemblance to 
 alteration forms, and I can not escape the conviction that the tendency 
 of future studies will be to attribute a secondary origin to more and 
 more of such intergrown brown hornblende. 
 
 The derivation of fibrous or actinolitic hornblende, quite identical in 
 all respects with uralite, from compact hornblende (whether brown or 
 green) seems hitherto to have been much neglected. luostrauzeff in 
 1879 described Russian diorites in which the original hornblende had 
 passed into secondary aetinolite, as well as into biotite, chlorite and 
 talc. 8 Becke also, in 1882, mentions uralite formed from both pyroxene 
 and compact, primary hornblende, in the kersantite of the “Nieder- 
 oesterreicliisckes Waldviertel.” 9 
 
 Descriptions have also been given by myself of compact brown horn- 
 blende changing into the green fibrous variety in the Baltimore 
 gabbros. 10 
 
 1 Verli. (1. naturh. Vereins d. pr. Rlieinl. und Westf., 1878, p. 171, pi. iv, fig. 4. 
 
 2 Die-Diabase des oberen Rulirthals, etc., Inaugural-Dissertation. Bonn, 1884, p. 41. 
 
 3 Quart. Jour. Geol. Soc. London, vol. 41, p. 137, 1885, pi. II, fig. 2. 
 
 4 T7eber die Entsiehung der altkrystallinischcn Schiefergesteine, etc. Bonn, 1884. 
 
 6 Jahrbucli preuss. geol. Landesanstalt fiir 1884, p. 537, Berlin, 1885. 
 
 6 Mikros. Pliysiog., 2d ed., vol. 2, 1887, pp. 141, 209. 
 
 7 TJeber kryst. Gest. Bosniens und der Herzegovina in Grundlinien der Geol. von Bosnien -Herzego- 
 vina, Wien, 1880 (ref. Nenes Jahrbucli fiir Mineral., 1881, vol. 2. Referate, j>. 353). 
 
 8 Studien fiber inetainorphosirte Gesteine im Gouvernement Oloncz. Leipzig, 1879 ( cf . Neues Jabr- 
 bucli fiir Mineral., 1880, vol. 2. Referate, p. 342). 
 
 9 Tschermak’8 mineral, u. petrog. Mittheil., vol. 5, 1883, pp. 157-159. 
 
 10 Bull. U. S. Geol. Survey, No. 28, p. 45. 
 
WILLIAMS.] 
 
 CHLOR1TIZATION. 
 
 55 
 
 The common alteration of rock-forming hornblende appears to be to 
 chlorite or to epidote, or into an aggregate of both these minerals. 
 This is almost the only change mentioned by Rosenbusch in his most re- 
 cent works, although in one place he says : il * * * bei Chloritisirung 
 
 fasert sicli die Hornblende aus * * * ” etc . 1 That this change of 
 compact to fibrous hornblende is, however, of great importance, the rocks 
 described in the sequel will abundantly prove. 
 
 Chloritization. — An admirable exposition of the present state of our 
 knowledge relative to the so-called “chloritic constituent” of the dia- 
 bases and allied rocks is to be found in the most recent work of Rosen- 
 busch . 2 The secondary hydrous minerals of a green color, whose almost 
 universal presence has brought to this whole class of rocks the gen- 
 eral designation ‘‘greenstone,” owe their existence to the processes 
 known as weathering, rather than to such as may be strictly called met- 
 amorphic. There can be but little doubt that they have been formed 
 mainly out of the components of the pyroxene, although these wander 
 so during the process of the alteration that the new products by no 
 means occupy the exact position of the original mineral. It seems pos- 
 sible to distinguish two classes of such secondary substances : First, 
 such as are more or less fibrous in structure, without pleochroism, and 
 have a decided action upon polarized light; and, second, such as are 
 scaly in structure, with pleochroism and so weakly polarizing as to 
 appear isotropic. The first class embraces substances allied to serpen- 
 tine; the second, those which more or less closely resemble chlorite. 
 In certain cases they have been chemically identified with such indefi- 
 nite species as delessite,grengesite (Hisinger), seladonite, chloroplneite 
 (Macculloch), epichlorite (Rammelsberg), diabantachronnyn (Liebe ), 3 
 and diabantite (Hawes ). 4 All of these substances resemble each other 
 more or less closely in both physical and chemical behavior, and I am 
 inclined to agree with Rosenbusch 5 in preferring the generic term 
 u chlorite ” or “ chloritic substance ” for them, to even the indefinite des- 
 ignations “ viridite ” of Vogelsang 6 or u chloropite” of von Giimbel. In 
 fact Keungott has shown that the formula of diabantachronnyn may 
 be brought quite into accord with that of typical chlorite . 7 
 
 Liebe found the greenish coloring-matter of the dark titanic iron 
 diabases of Voigtland and Frankenwald to be picrolite (serpentine), and 
 it is not unusual to observe the curious vermicular aggregates of cir- 
 cular chlorite scales to which Volger has given the name helminth . 8 
 
 It is well known that the results produced by the weathering of horn- 
 
 1 Mikros. Physiog., 2d ed., vol. 2, 1887, pp. 468,469. 
 
 2 Ibid., pp. 180-184. 
 
 *Neues Jahrbuch fur Mineral., 1870, p. 2. 
 
 4 Am. Jour. Sci., 3d series, vol. 9, 1875, pp. 454-457 ; Geol. Now Hampshire, vol. 3, part 3 ; 1878, p. 120. 
 
 6 Mikros. Physiog., 2d ed., vol. 2, 1887, p. 183. 
 
 c Archives N6erlandaisos, vol. 7, 1872; Zcitscb. Deutsch. geol. Gesell., vol. 21, 1872, p.529. 
 
 7 Neues Jabrbuch fiir Mineral., 1871. p. 51. 
 
 8 Studien zur Entwickeluugsgeschichto der Mineralion, 1854, p. 142. 
 
56 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 blende or mica are, in most instances, quite similar to those just de- 
 scribed in the case of pyroxene. Such a change of hornblende may have 
 an equal importance in those greenstones, like a large proportion of 
 those to be considered in this paper, whose bisilicate constituent was 
 originally augite, but which was subsequently changed by a truly meta- 
 morphic process (uralitization) to hornblende before the final weather- 
 ing commenced. 
 
 The last result of the action of the atmospheric influences upon the 
 chlorite is, as Rosenbusch long ago showed, to convert it into an aggre- 
 gate of limonite, carbonate, and quartz. 
 
 Epidotization . — The most careful and detailed observations on this 
 process are to be found in the Inaugural Dissertation of Adolf Sehenck 
 on the Diabases of the upper Ruhr Valley and their Contact Phenom- 
 ena. 1 This investigator finds that certain of these diabases are converted 
 into u Epidosites,” or aggregates of epidote and either quartz or calcite. 
 He suggests the only three possible hypotheses for the formation of 
 this epidote, viz: (1) That it was formed by the action of the decomposi- 
 tion products of the bisilicate (mainly CaO and Ee 2 0 3 ) upon the feld- 
 spar substance ; (2) That the reverse was true, i. e., that the decomposi- 
 tion products of the feldspar (mainly A1 2 0 3 and CaO) acted upon the 
 pyroxene ; (3) That there was a mutual reaction between the decom- 
 position products of both the original constituents. The first of these 
 hypotheses is regarded by the author as the only tenable one for the 
 rocks which he studied, because in all those diabases which contained 
 much epidote the feldspar was remarkably fresh and the pyroxene de- 
 composed, while in those whose feldspar was extensively altered epidote 
 was almost wanting. Observations of the change of feldspar to epidote 
 are cited from the writings of Dathe, Cohen, Rosenbusch, Liebisch, von 
 Lasaulx, Inostranzeff, Zirkel, Michel Levy, Kuhn and Scheilitz; and even 
 more authorities are quoted to show that this same mineral originates 
 from augite, or more commonly from hornblende or uralite. If iron is 
 not at hand, the place of the epidote appears to be taken in the feld- 
 spar by zoisite. An excellent example of the origin of epidote as a re- 
 actionary rim between the substance of hornblende and plagioclase has 
 been described and figured by myself in the Baltimore gabbros and their 
 derivatives. Here the epidote forms a continuous border around the 
 hornblende, it s crystals projecting from it outward into the feldspar 2 
 
 Viridite (chlorite)- Epidote Aggregate . — The simultaneous action of the 
 two last described processes (chloritization and epidotization) in an 
 aluminous pyroxene or hornblende results in the production of an ag- 
 gregate consisting of sharply defined, pale yellow crystals of epidote, 
 imbedded in a green, scaly mass of chlorite. The appearance of this 
 under the microscope is shown on PI. XI, fig. 1. The magnesia, together 
 
 *Die Diabase des obercn Rulirthals und ibro Contacterscheinuugen mit dem Lenneschiefer. Bonn, 
 1884. 
 
 2 Bull. U. S. Geol. Survey, No. 28, 1880, p. 32. PI. m, Fig. 2. 
 
WILLIAMS.] 
 
 THE CHLORITE EPIDOTE AGGREGATE. 
 
 57 
 
 with a proportion of the iron, alumina and silica, have here formed 
 the chlorite; while the lime, instead of becoming a carbonate, as it often 
 does, has become fixed, in combination with the rest of the iron? 
 alumina and silica, as epidote. 
 
 Such aggregates have not escaped the notice of petrographical stu- 
 dents, though curious mistakes have sometimes arisen as to their true 
 nature and origin. 
 
 In 1874 Dathe described this association of chlorite and epidote with 
 great correctness and precision. He says : 
 
 When secondary products become abundant and the leek-green viridite increases 
 in amount and distribution, then there are often associated with this light yellow 
 crystals, whose difference from the viridite is very apparent under the microscope. In 
 the progress of my studies, I have recognized these crystals as pistazite . 1 
 
 In 1876 Zirkel described the change of horu blende to an aggregateof 
 epidote, viridite (chlorite) and magnetite, with which, in many instances, 
 more or less cal cite was associated. 2 
 
 In the same year, Wichmann, in his paper on the iron rocks of the 
 south shore of Lake Superior, which was not, however, published until 
 1880, 3 described this chlorite epidote quite correctly in some instances, 
 although he says that it is beyond doubt that the epidote has been formed 
 out of the viridite. In other cases he regards the mineral imbedded in 
 the viridite as a secondary augite, which, as in the last instance, he 
 thinks was formed from the chlorite. He says of this : 4 
 The phenomenon of the transformation of viridite into augite has not been observed 
 until recently. It is very interesting to have the fact established that this mineral, 
 after having been changed into another, has finally returned to its former state. * * * 
 Such individuals are only present in viridite and do not seem to occur in any other 
 part of the rock. 
 
 George F. Becker in the course of his microscopical studies of the 
 rocks of the Comstock Lode, ^Nevada, which were either identical with 
 those investigated by Zirkel, or very closely allied to them, found the 
 same change of bisilicates to an aggregate of chlorite and epidote which 
 the latter observer had recorded. Mr. Becker is, however, very posi- 
 tive that the epidote has been developed after and at the expense of the 
 chlorite, instead of simultaneously with it. 5 This he attempts to explain 
 upon chemical grounds. 6 The improbability of Becker’s supposition 
 was brought out by Rosenbusch in a review of his work. 7 
 In this, as well as in his more recent text-book, 8 Rosenbusch clearly 
 
 1 Wenn die Neubildnngsproducte sich im Gestein haufen, wenn der lauchgriine Viridit [ChloritJ an 
 Masse und Verbreitung zunimmt, stellen sich oftmals neben letztoren lichtgelbliche Gebilde ein, 
 deren Verscliiedenheit vom Viridit bei mikroskopischer Betracbtung sofort in dio Augen springt. Ira 
 Verlauf der Untorsnclrang wurdeii diese Gebilde als Pistazit erkannt. Mikroskopischo Unter 
 snehungen iiber Diabase. Zeitsch. Dentsch. geol. Gesell., vol. 26, 1874, p. 16. 
 
 ^Microscopical Petrography, Washington, 1876, p. 66, PI. ill, Figs. 2 and 3. 
 
 3 Geol. Wisconsin, vol. 3, 1880, pp. 600-656. 
 
 « Ibid., pp. 623, 624. 
 
 “The Geology of the Comstock Lode. Monograph U. S. Geol. Survey, vol. 3, p. 76. 
 
 6 Ibid., pp. 211-214. 
 
 7 Noues Jahrbuch fiir Mineral., 1884, vol. 2. Referate, p. 189. 
 
 ®Mikros. Physiog., 2d ed., vol. 2, pp. 108, 183. 
 
58 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 shows that the true deviation of the chlorite-epidote aggregate is to 
 be found in a division of the bisilicates out of w T hich it is formed, 
 the magnesia passing into the chlorite and the calcium and ferric iron 
 into the epidote. The triclinic feldspar may often materially assist in 
 this formation by furnishing the necessary lime. 
 
 Nor is this mistake of Mr. Becker's a new one. Francke in 1875 de- 
 scribed the same mineral association and gave the same explanation for 
 it; 1 while in 1880 Schauf, 2 in 1882 Kiemann, 3 and in 1884 Schenck cor- 
 roborated the observation, although both Schauf and Schenck 4 raised 
 unanswerable chemical objections to the derivation of the epidote from 
 the chlorite. 
 
 Saussuritization. — The hard, compact, whitish or greenish substance, 
 without luster or cleavage, which forms one of the two main components 
 of the certain coarse gabbros or euphotides, was called by H. B. Saus- 
 sure, in 1780, “jade.” 5 In 180G Th. Saussure named this mineral, in 
 honor of his father, “saussurite, 6 but its true nature continued for over 
 half a century to elude all mineralogists. As long as chemical analysis 
 was the only means with which it could be studied, any satisfactory 
 solution of the riddle seemed to be impossible. Such investigators as 
 vom Bath, 7 Klaproth, 8 T. Sterry Hunt, 9 and many others obtained the 
 most diverse results; the composition in some cases approaching that 
 of zoisite, in others that of garnet, scapolite, or feldspar. In 186G, Zir- 
 kel remarked, at length, upon the extremely imperfect state of knowl- 
 edge regarding this geologically important mineral. 10 
 
 It remained for the microscope to disclose the composite nature of 
 saussurite as well as to point out the true significance of its origin and 
 occurrence. 
 
 Hagge was the first to correctly describe saussurite as an aggregate of 
 colorless or greenish crystal needles, prisms or grains, irregularly scat- 
 tered through a colorless, glassy-looking matrix. 11 He, however, retained 
 the name saussurite for the included grains, and did not attempt to de- 
 termine their mineral nature. Hagge.also clearly recognized that in all 
 cases observed by him the saussurite was a product of the alteration of 
 feldspar, and that the passage from one mineral to the other was a grad- 
 ual one which the microscope could easily follow. 12 These results were 
 
 1 Studien iiber Corillerengesteine. Inaugural-Dissertation. Leipzig, 1875. 
 
 2 Verhl. d. nat. Vereins d. pr. Rheinl. u. Westf., 1880, p. 6. 
 
 3 Ibid., 1882, p. 256. 
 
 4 Inaugural-Dissertation. Bonn, 1884, p. 45. 
 
 E Voyages dans les Alpes, vol. 1, Neuch&tel, 1779, p. 83. 
 
 6 Annales de chirnie et de physique, 3d series, vol. 16, p. 469. 
 
 7 Poggen ( lovfF Annalen, vol. 95, 1855, p. 555. 
 
 8 Beitrage, vol. 4, p. 271. 
 
 9 Am. J our. Sci., 2d series, vol. 27, 1 859, pp. 336-349. 
 
 10 Lelirbucli der Petrograpbie, vol. 1, p. 27 ; vol. 2, p. 110, 1866. 
 
 I] Mikroskopiscbe Untersuchungen iiber Gabbro and vorwandte Gesteino. Kiel, 1871. On p. 51 ho 
 says: “ Der Saussurit besteht aus kleinen Krystallnadelu, Prismen uml Kbrneru, die tarblos oder 
 blassgriin sind und rogellos in einer wie ein farbloses Glas aussehenden Grundmasse, die aucli viel- 
 facli klare Spalten in dem Saussurit bildot, vertbielt liegeu.” 
 
 12 Ibid., pp. 35 and 51. 
 
WILLIAMS.] 
 
 SAUSSUR1TIZATI0N. 
 
 59 
 
 quoted by Zirkel in liis text- book, published in 1873. 1 The conclusion 
 that saussurite was “an aggregate and probably the end product of a 
 molecular rearrangement in the feldspar” was also reached by Rosen- 
 busch in the same year. 2 In 1878 Becke showed that the saussurite of 
 certain Grecian rocks was largely zoisite ; 3 and in 18S3 appeared the im- 
 portant paper by Oathrein upon this subject. 4 This author draws from 
 his work the following six conclusions as to the nature of saussurite. 
 
 (1) The so-called saussurite, far from being a homogeneous mineral, 
 is an aggregate of plagioclase, rarely orthoclase, with zoisite. Actino- 
 lite, chlorite, and other minerals may also occur as accessories. 
 
 (2) The chemical composition of saussurite resembles most that of 
 the lime soda feldspars ; it, however, contains less silica, more lime, and 
 has a higher specific gravity. 
 
 (3) ' The proportions of the saussurite elements can be calculated from 
 the amounts of alkalies, lime, and iron, if we know the species of the 
 original feldspar. 
 
 (4) This proportion can also generally be calculated, even when this 
 last factor is unknown, by a consideration of the relative difference of 
 silica, alumina and lime in zoisite and anortiiite. 
 
 (5) Saussurite is a product of the metamorphism of feldspar through 
 an exchange of silica and alkali for lime, iron and water. 
 
 (6) The epidotization of feldspar is genetically the same process as 
 saussuritizatiou and differs only in the larger proportion of iron required. 
 
 H. Reusch considered the saussurite which composed a large part of 
 the Bergen gabbros as partly epidote, partly zoisite. 5 Traube found 
 the structure and composition of the saussurite occurring in the gab- 
 bros of Lower Silesia to be like that described by Oathrein, 6 while 
 Brogger mentions neither epidote nor zoisite, but regards some mem- 
 ber of the scapolite family as probably present in the saussurites studied 
 by him. 7 Paul Michael has recently investigated the saussurite-gabbros 
 of the Fichtelgebirge in Bavaria and concludes that two main types of 
 saussurite occur there. One of these consists mainly of zoisite, with 
 more or less alkaline feldspar, and the other is composed of a pale lime 
 alumina garnet together with serpentine. 8 
 
 J. Lehmann 9 and Lossen 10 were the first to recognize in the saussur- 
 itization of feldspar a result of dynamic or regional metamorphism — an 
 idea which Rosenbusch has lately more clearly developed and elabo- 
 
 1 Die mikroakopische Beachaffenheit der Mineralion uud Gesteino. Leipzig, 1873, p. 143. 
 
 2 Die petrographiscli wichtigen Mineralien, 1873, p. 356. 
 
 3 Tscliermak’s mineral, u. petrog. Mittheil., vol. 1, 1878, p. 247. 
 
 4 Zcitsclir. Kryst., vol. 7, 1883, p. 234. 
 
 6 Die fossilien-fiihrcnden krystallinischen Sckiefer von Bergen in Norwegen. German translation by 
 Baldauf, 1883, p. 40. 
 
 6 Beitriige znr Kenntniss der Gabbros, Amphibolite und Serpentino des nieder-sclilesisclien Gebirgos. 
 Inaug.-Disser., 188 1, pp. 7,20. 
 
 7 NytMag. for Xaturvidouakaberne, vol. 28, 1884, p. 253. 
 
 8 Nones Jahrbucb fur Mineral., 1888, vol. 1, pp. 36-41. 
 
 9 Untersuchungen iiber die Eutstehuug der altkrystallinischen Scbieforgestoinc, etc. Bonn, 1884, 
 
 pp. 197, 199. 
 
 ,0 Jahrbuch k. preuss. geol. Laudesanstalt fiir p. 
 
60 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62 . 
 
 rated . 1 This last-named authority shows that the new mineral devel- 
 oped in the feldspar is by no means always of necessity zoisite or epi- 
 dote. It may also be garnet, or a miueral of the scapolite family. He 
 remarks : 2 
 
 The sura total of these new products, which are certainly not produced by normal 
 weathering, but are due to a raetamorphic process, we designate as the saussuritiza- 
 tion of feldspar . 3 
 
 Michel-Levy was the first to show that the so called “ spotted-gab- 
 bro (gefleckter Gabbro) of Brogger and Reusch was a mixture of arn- 
 phibole and wernerite ; 4 * and Sjogren has since demonstrated that the 
 latter mineral is secondary to feldspar, and the first to pyroxene. 
 Fouque and Michel-Levy tried the interesting experiment of fusing this 
 rock, and obtained therefrom an aggregate of pyroxene and labradorite . 6 
 
 Formation of the Albite Mosaic. — Analogous and closely related to 
 the saussuritization of feldspar are cases where, in the process of its 
 alteration by metamorphism, the lime is more or less completely re- 
 moved or crystallized as cal cite, instead of forming a calcium silicate. 
 In such instances the alkaline portion of the plagioclase molecule crys- 
 tallizes in the form of a finely granular aggregate, or mosaic of limpid 
 grains (albite). These may be wholly devoid of twinning lamellae and 
 often closely resemble quartz, with which they are not infrequently 
 associated. Of course such mosaics are connected by every stage of 
 transition with saussurite, according as more or less of the lime has re- 
 mained as a calcium silicate (zoisite or epidote). 
 
 Such a granulation of the feldspar substance has already been 
 alluded to under the head of mierostructural metamorphism; but, inas- 
 much as a complete solution and recrystallization of clear feldspar sub- 
 stance often takes place, it belongs quite as much to this division of the 
 subject. The geological significance of this method of feldspar altera- 
 tion, especially in certain basic eruptive rocks like diabase, has been most 
 persistently emphasized by Lossen. He has shown how it may result 
 in the total obliteration of the original and characteristic rock-struct- 
 ure, and how, therefore, it may prove most misleading, unless its nat- 
 ure and origin are clearly understood . 7 J. Lehmann , 9 Teal l , 8 and others 
 have also observed and commented on such a secondary feldspar 
 mosaic. 
 
 Sericitization. — The soft, unctuous mineral characteristic of so many 
 slates and schists was formerly regarded as talc. This gave rise to the 
 
 ‘Mikros. Physiog.,2d eel., vol. 2, 1886, p. 164. 
 
 2 Ibid., p. 137. 
 
 3 “Die Gesammtheit dieser Neubildungen, die sicherkeine Art der normaler Vorwitterung, sond6rn 
 ein metamorpher Vorgang ist, bezeicknet man als die Saussuritisirung des Feldspatha.” 
 
 4 Bull. Soc. Mineral, de France, vol. 1, 1878, pp. 43, 79. 
 
 fi Geol. Foreningena Stockholm Fdrbandl., vol. 6, 1883, p. 447 (Neues Jahrbuckfiir Mineral., 1884, vol. 
 1, referate p. 81). 
 
 6 Bull. Soc. Mineral, de Franco, vol 2, 1879, p. 105. 
 
 7 Jalirbuck preuss. geol. Landesanstalt fur 1883, p. G40 PI. 29 ; ibid., 1884, pp. 525-530, PI. xxix, Figs. 
 2 and 4. 
 
 8 Uutcrsuchungcn iiber die Entstekung der altkrystalliniscken Scbicfergeatoine, etc., 1884, p. 207. 
 
 9 Quart. Jour. Geol. Soc. London, vol. 41, 1885, p. 139. 
 
WILLIAMS.] 
 
 SERICITIZATION. 
 
 61 
 
 common designation “soapstone” or “talcose slates,” which was used 
 very early in America by Amos Eaton. 1 As early as 1819, however, 
 Prof. Chester Dewey, of Williams College, made the statement that he 
 was able to detect very little magnesia in the specimens which, he ex- 
 amined, while alumina was abundant. He therefore preferred to call 
 these rocks micaceous slates. 2 
 
 In Europe, slates of this kind were first studied from the Taunus, 
 where they were usually regarded astalcose until 1847, when Sandber- 
 ger made the same discover that Dewey had made with regard to the 
 American rocks. 3 List subsequently studied more carefully this mica- 
 ceous constituent of the Taunus schists, and named it, on account 
 of its silky luster, u Sericite.” 4 Scharff attacked the conclusions of List 
 and considered sericite to be only a mixture, 5 while Lossen vigorously 
 defended the individuality of the mineral. 6 
 
 The sericite was soon identified by many investigators in the rocks 
 of many regions. 7 Prof. Dana united it with the species margaro- 
 dite and damourite in the group of hydro-micas and called this class 
 of slates the hydro-mica slates. Of these so-called hydro-micas Prof. 
 Dana says : 
 
 The following species [margarodite, damourite, paropliite, sericite, sericite schist, 
 groppite, enphyllite, cookeite, voigtite, roscoelite,] are mica-like in cleavage and as- 
 pect, but talc-like in wanting elasticity, in greasy feel, and in pearly luster. They 
 are sometimes brittle. Common mica, muscovite, readily becomes hydrated on ex- 
 posure ; but hydrous micas are not all a result of alteration. Hydro-mica schists 
 form extensive rock-formations, equal to those of the ordinary mica-schists . 8 
 
 In 1880 Laspeyres made a very thorough examination of sericite 
 and showed conclusively its identity with muscovite. 9 It differs from 
 the ordinary form of this species only in its compact structure and in 
 its geological significance; but, since both of these are characteristics, 
 there is a decided advantage in retaining the name sericite, especially 
 in petrography, to designate a peculiar form and occurrence of musco- 
 vite. 
 
 The alteration of orthoclase into kaolin or clay was very early known. 10 
 The corresponding change of the same feldspar into mica, was first ob- 
 served by Haidinger in 1841, 11 but was subsequently found to be not 
 
 I Index to the Geology of the Northern States, pp. 147, 174, 28G. 
 
 * Am. Jour. Sci. 1st series, vol. 1, 1810, p. 310. Thus the discovery, usually attributed to Sandberger, 
 was anticipated in America by twenty-eight years. Cf. Dana's Manual of Geology, 3d ed., p. 72. 
 
 3 Uebcrsicht d. geol. Vorhaltnisso d. Horzogth. Nassau, 1847, p. 94. 
 
 •*Jahrb. d. Vereinsf. Naturkundo im Horxogth. Nassau, vol. G, 1850, p. 126; vol. 7, 1851, p. 266; vol. 
 8, 1852, p. 128; Annalen Chem. und Pharni., vol. 81, 1852, p. 181. 
 
 6 Neues Jabrbucli fur Mineral., 18C8, p. 309 ; ibid., 1874, p. 271. 
 
 6 Zeitschr. Deutseh. mineral, geol. Geasell., vol. 19, 1867, p. 509; vol. 21, 1869, p. 281. 
 
 7 e. g., by Pichler in the Tyrol. Neues Jahrhueh fur Mineral., 1871, p.56 ; by Tornebohm in Sweden, 
 Neues Jahtbnch fur Mineral., 1874, p. 141 ; by von Laaaulx in the Ardennes; by Credner in Saxony 
 and by Wicbmanu in the Lake Superior rocks. 
 
 8 Manual of Mineralogy and Petrography. 4th ed. New Vork, 1887, p. 335. 
 
 9 Zeitschr. Kryst., vol. 4, 1880, pp. 244-256. 
 
 10 Blum : Psetidomorphosen d. Mineralreichea, 1843, p. 72. 
 
 II Abli. d. k. bblim. Geaell. d. Wisaunachaft, 1841, p. 4. Bluui: Paeudomorphosen, Nuchtr., 1, 1847, 
 
 p. 25. 
 
62 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 {bull. 62. 
 
 uncommon. Since rocks have been studied with the microscope, the 
 change of potash feldspar to muscovite or sericite has been found to 
 possess a wide significance, especially in dynamic metamorphism. 
 
 There seems every reason to believe that sericite always originates 
 from potash feldspar and not from other micas. Its constant and very 
 intimate association with quartz shows, as first pointed out by Las- 
 peyres, 1 that it was derived from an acid silicate. 
 
 Any rocks, therefore, whether sedimentary or massive, which con- 
 tain orthoclase, may give rise to sericite ; but its formation, in any case- 
 would seem to require the action of some great dynamic force. The 
 close relation between dislocation and mica formation, so clearly illus, 
 trattd by J. Lehmann, 2 is in an eminent degree applicable to sericite. 
 It is now a well known and oft-recorded fact that in any rock mass, 
 where the strains and stresses have been the most intense, there the 
 micaceous minerals are most abundant ; and if the rocks are orthoclas- 
 tic these will be largely sericite. Sericitization is therefore a phenome- 
 non of dynamic metamorphism. It is in a way, as Lehmann says, a 
 retrogressive metamorphic process, since feldspar is by it not formed, 
 but destroyed. It is also the most extreme manifestation of dynamic 
 action in orthoclase rocks and may produce the same result — a sericite 
 schist — from a clastic arkose on the one hand, and from a massive gran- 
 ite or quartz-porphyry on the other. 3 
 
 In an admirable paper on the paragenesis of certain ore deposits, A. 
 von Groddeck has shown that the rocks, heretofore considered as tal- 
 cose, which occur near Holzappel and Werlau on the Bhine, at Mitter- 
 berg in Salzburg and at Agordo in the Venetian Alps, are iu reality 
 sericite schists. These he considers to represent the extreme phase of 
 metamorphism, in some cases of an eruptive rock (diabase), and in other 
 % cases of a normal clay state or graywacke. 4 It seems most probable 
 that these rocks owe their origin to dynamic agencies, with which the 
 deposition of the ore also stands in close relationship. 
 
 The alteration of the feldspathic groundmass of quartz porphyries 
 to muscovite or sericite, especially where these have been rendered 
 schistose by pressure, is now well known. In this way porphyroids 
 may be derived from massive eruptive rocks. In the more massive 
 quartz porphyries studied by 0. Schmidt from the central Alps (Wiud- 
 gallen), sericite is met with as an occasional pseudomorph after the 
 feldspar, but in the schistose porphyries derived from the latter by pres- 
 sure and stretching, this mineral is much more abundant ; so abundant, 
 indeed, as, in some instances, to make up, along with quartz, the whole 
 mass of the rock. 5 6 
 
 ‘Zeitschr. Kryst., vol. 4, 1880, p. — . 
 
 2 Unter8uc1iungen iiber die Entstehung der altkrystallinisclien Schiefergestoine. Bonn, 1884. Cap. 
 IX. Druckscliieferung und Glimmerbildung, p. 136. 
 
 •Ibid., p.101. 
 
 4 Zur Kenntniss ciniger Sericitgestoine, -welch© neben undin Erzlagerstatten auftreten. Neues 
 
 Jahrbuch fiir Mineral., Beilage-Band 2, 1883, pp. 72-138. 
 
 6 Neucs Jahrbucb fiir Mineral., Boilage-Band 4, 1886, p. 428. 
 
WILLIAMS.] 
 
 LEUCOXENE. 
 
 63 
 
 Alterations of titanic iron . — The element titanium exists in unaltered 
 diabases almost exclusively in combination with iron as ilmenite or as 
 titaniferous magnetite. In the processes of metamorphism, however, 
 various other titanium compounds are formed. The most common phase 
 of this change consists in the development of a gray rim around the 
 the ilmenite grains. This substance is also often seen along the rhom- 
 bohedral cleavage cracks of the ilmenite, giving rise to the well known 
 gridiron structure so often figured. 1 There can be no doubt that this 
 gray material is an alteration product of the ilmenite, although Giimbel, 
 who gave it its name, leucoxene , regarded it as a parallel growth of 
 another mineral. 2 Much difference of opinion formerly prevailed in 
 regard to the chemical nature of the leucoxene. Zirkel at first regarded 
 it as iron carbonate, 3 Cohen as titanic oxide, 4 Rosen busch as anatase. 5 
 Giimbel regarded it as probably a titanosilicate, while both Fouque 6 
 and Michel-Levy 7 thought that it was a form of sphene. The identity 
 of both leucoxene and titano-morphite (another similar substance 
 described by von Lasaulx around the rutile of an amphibolite from 
 Lampersdorf in Silesia) 8 with titanite or sphene was first conclusively 
 proved by A. Cathrein in 1882. 9 
 
 The freqnent passage of the dull gray leucoxene rim into clearly de- 
 fined aggregates and crystals of sphene is mentioned by Cathrein, 10 and 
 the origin of sphene by the alteration of ilmenite is also described by 
 W. C. Brogger. 11 Fine examples of this origin for sphene are also 
 described and figured in the sequel. 
 
 Anatase has been described as an alteration product of ilmenite, by 
 Differ. 12 
 
 The rutile needles frequently seen about ilmenite, either with or 
 without leucoxene, are regarded by Cathrein as an original intergrowth 
 of this mineral with the ilmenite. 13 Further reference will be made 
 hereafter to needles of this character occurring in some of the Menom- 
 inee greenstones. 
 
 *Cf. Valloo'do la Poussin et Renard: Roclies plutoniennes de la Belgique, etc., 1874, PI. VI, Figs 31 
 
 and 32. 
 
 2 Palseolithische Eruptivgesteine des Fichtelgebriges, Munich, 1874, p. 35. 
 
 * Mikroskopischo Beschaffenheit d. Min. u. Gest., 1873, p. 409. 
 
 4 Erliiaternde Bemerkungen z. d. Routenkartc, etc., 1875, p. 55. 
 
 5 Mikros. Physiog., 1st ed., vol. 2, 1877, p. 336. 
 
 e Cours do College do France, 1877. 
 
 7 Bull. Soc. G6ol. France, 3d series, vol. 6, 1878, p. 163. 
 
 "Neues Jahrbuch fur Mineral , 1879, p.568. 
 
 *Zeitschr. Kryst. u. Min., vol. 6, 1882, p. 244. 
 
 10 Ibid. 
 
 11 Nyt Mag. for Naturvidenskaborne, vol. 27, 1884, p. 359. 
 
 12 Neues Jahrbuch fiir Mineral., 1883, vol. 1, p, 193, 
 
 >* Zeitschr. Kryst. u. Min., vol. 6, p. 256. 
 
CHAPTER II. 
 
 GREENSTONE BELTS OF THE MENOMINEE IRON DISTRICT. 
 
 INTRODUCTORY AND HISTORICAL. 
 
 The exact geographical position of the two greenstone-schist areas 
 of the Menominee region are fully indicated in the explanatory and 
 historical note by Prof. Irving at the beginning of this memoir 
 and upon the accompanying geological map of this district. (PI. II). 
 The same note explains and discusses the different views which have 
 been held by various geologists in regard to the stratigraphical position 
 of these greenstone schists in the general succession of the stratiform 
 rocks of the Menominee region. 
 
 A brief mention of the opinions which have already been published 
 regarding the petrographical character of these greenstone schists 
 is, however, desirable. 
 
 The first attempt to describe the Menominee greenstones and green- 
 stone schists lithologically was made by Hermann Credner in i860, 
 from observations collected while he was acting as assistant to Prof. 
 Pumpelly on a survey for the Portage Lake and Lake Superior Ship 
 Canal, during the years 1867- C8. 1 In his first paper entitled Die vorsi- 
 lurischen Gebilde der oberen Halbinsel von Michigan in Nord-Amerika , 2 
 Credner gives a section of the strata of the Menominee Iron Region, 
 commencing with the oldest member, from which the following is abbre- 
 
 viated : 
 
 Feet. 
 
 a. Quartzite 8,000 
 
 1). Crystalline dolomitic limestone 3,500 
 
 c. Red Iron ore 600-1,000 
 
 d. Chlorite schist 1, 000-1, 500 
 
 e. Clay slate 8,500 
 
 /. Chlorite schist with diorite 1,200-1,400 
 
 g, h, i, k. Talc schist 150 
 
 l. Dioritic series „ 2,300 
 
 m. Talcose clay slate 1,500 
 
 The members / and l are evidently parts of the same formation, in 
 which the beds g , h , i, and h are interstratified. In his description of 
 /, Credner says : 
 
 In the upper horizon of this series there occur beds of fine and coarse grained 
 diorite and aphanite, varying in thickness from ten feet to several hundred. These 
 
 64 
 
 1 See Geology of Michigan, vol. 1, 1873, p. 157, note. 
 
 2 Zeitachr. Deutsch. geol. Ge3cll., vol. 21, 1869, pp. 516-554. 
 
WILLIAMS. ] 
 
 WORK OF CREDNER AND BROOKS. 
 
 65 
 
 rocks consist mainly of dark green hornblende and white or pale green oligoclase, 
 with which granular or scaly chlorite is often associated. Crystals of pyrite and mag- 
 netite are also frequent. Indications of a lamellar parting are frequent, while rect- 
 angular jointing is rare. 1 
 
 In the same article, in speaking of the member £, the author says : 2 
 
 Dioritic series 2,300 feet in thickness. Mainly a fine grained or aphanitic, rarely 
 a coarsely crystalline aggregate of the constituents of diorite. All contain crystals 
 of pyrite ; the aphanite contains veins of calcite and quartz. 3 
 
 In a second, article entitled Ueber nor damer iJcanische tSchieferporphy- 
 roide , which also deals with certain rocks exposed on the Meuominee 
 River, 4 Oredner unites his beds / and l as “chlorite schist alternating 
 with intercalated diabase ; 77 while his g , h, i, and Jc are described as a 
 series of “ porphyroid-schists , 77 300 feet in thickness, between two beds 
 of diabase. 
 
 In the year 1869 the geological survey of Michigan was inaugurated 
 with the iron-bearing formations of the Upper Peninsula, in charge of 
 Maj. T. B. Brooks. The results of his labors appeared in 1873, 5 accom- 
 panied by two appendices, containing special petrographical descrip- 
 tions of the rocks collected by Julien, 6 and Wright. 7 Several of the 
 Menominee greenstones, both massive and schistose, come within these 
 descriptions, but the descriptions are for the most part vague; as, for 
 instance “diorite/ “dioritic schist/ “ porphyritic diorite/ etc. 
 
 In 1874 Major Brooks continued his studies of the Menominee region 
 under the auspices of the Wisconsin Geological Survey. The results 
 of this work appeared in 1879 8 and contained much more elaborate 
 and accurate determinations of the greenstones and greenstone schists. 
 Major Brooks gives a diagram 9 to illustrate his general views of the 
 observed transitions of greenstones (believed to be mostly metamor- 
 phosed sediments) into related rocks. Dr. Wichmanu, who furnished 
 the systematic petrographical descriptions of these rocks iu Brooks’s 
 report, 10 however, regarded these rocks as for the most part eruptive 
 and to a large extent as derived from diabase. Special reference will 
 be made to the descriptions of Wichmann and others who have worked 
 
 1 Zeitschr. Deutsch. geol. Gesell., vol. 21, 1869, p. 528. 
 
 7 Im oberen Horizonte dieser Schichtenreihe treten von 10 bis mehrere hundert Fuss macbtige Einla- 
 gerungen von fein- bis grobkoruigem Diorit sowie von Aphanit auf. Sie beetehen vorwaltend aus 
 dunkelgriiner Hornblende und weissem oder kellgriinem Oligoklas, wozu sich an mancben Pnnkten 
 viel kornig-scliuppiger Chlorit gesellt. Einsprenglinge von Schwefelkies und Magneteisenstein sind 
 iu ihnen haufig. Andeutung von plattenformiger Absonderung ist gewohnlich, quarderformige Ab- 
 aonderung selten. 
 
 * Ibid., p. 529. 
 
 4 Dioritische Gesteinsreihe von 2,300' Macbtigkeit. Vorwaltend ein feinkorniges oder aplianitiscbes, 
 seltener eiu grobkrystalliniscbes Gemenge der Bestandtbeile des Diorites, alle mit Schwefelkies ein 
 ein sprenglingen, die Aphanite ink; Schuiiren von Kalkspath und Quarz. 
 
 ‘ 6 Neues Jabrbuch fur Mineral., 1870, pp. 970-984. 
 
 ‘Geol. Survey Michigan, vol. 1, Upper Peninsula. Part I. Iron-bearing rock, by T. B. Brooks. 1873. 
 
 7 Ibid., vol. 2, 1873. Appendix A, Lithological descriptions, etc., of 259 specimens of the Huronian 
 and Laurentian of the Upper Peninsula, by A. A. Julien, pp. 1-197. 
 
 *Ibid., vol. 2, 1873. Appendix C. Microscopic determinations and descriptions of 78 specimens of, 
 Huronian rocks and ores, by O. E. Wright, pp. 213-231. 
 
 # Geol. Wisconsin, Vol. 3, 1873-1879. The Geology of the Menominee Iron Region, Oconto County, 
 by T. B. Brooks, pp. 429-663. Ibid , Geol. Menominee Region by C. E. Wright, pp. 065-741, 
 
 ,0 Ibid., 519. "Ibid., pp. 000-656, 
 
 Bull. 62- — 5. 
 
66 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 upon the petrography of the Menominee greenstones in the course of 
 the following chapters of this work. 
 
 All observers seem to be agreed that the association of the massive 
 greenstones with those which are more or less perfectly schistose is an 
 extremely intimate one. Even Major Brooks, in spite of his idea that 
 most of the greenstones are altered sediments, is constantly suggesting 
 the possibility of a mechanical origin for the intercalated schistose lay- 
 ers. He says 1 of the Twin Falls exposure : 
 
 This slaty material may be simply a compacted form of the pulverized greenstone 
 produced at the time of Assuring. 
 
 Again , 2 in speaking of the Commonwealth aud Eagle Mine rocks: 
 
 It will be observed that these rocks have some resemblance to aa, but it is be- 
 lieved that they are associated schistose and altered varieties of the great greenstone 
 bed XVIIL so extensively developed to the north and east. 
 
 He says 3 also: 
 
 An unevenly splitting, gray-green schist associated with greenstones and appar- 
 ently derived from them by alteration of the amphibole, is included in this family 
 (chlorite schist], although its origin and associations are widely different from the 
 above. 
 
 Again : 4 
 
 One of the largest, most generally distributed, and at the same time, obscure va- 
 rieties embraces those chloritic rocks that are associated with greenstones. 
 
 Dr. C. Kominger, in his Report on the Geology of the Menominee 
 Iron Region , 5 is equally impressed with the close association of the 
 massive aud schistose varieties of the greenstones. Like Brooks, he 
 regards them as of sedimentary origin, and thinks that the massive 
 portions are the result of extreme metamorphism, having recrystallized 
 from a partially fused state. 
 
 There seem to be only three different ways of explaining the facts as 
 they are plainly and abundantly manifested at each of the several points 
 examined on the Menominee River. 
 
 We may suppose, as did Foster and Whitney, Whittlesey and Cred- 
 ner, that the schistose portions of the rocks exposed at these several 
 points are more or less perfectly metamorphosed sedimentary material, 
 while the more massive portions represent intercalated beds of eruptive 
 origin. 
 
 We may imagine, on the other hand, as did Rominger and Brooks, 
 that all of these rocks, including the most schistose aud the most mas- 
 sive phases, are probably altered sedimentaries; supposing, with Romin- 
 ger, that the more massive kinds are merely the same sedimentary mate- 
 rial fused by the intensity of the metamorphosing action so as to lose all 
 trace of the original stratification ; or admitting, with Brooks, the possi- 
 bility, though great improbability, that some of the more massive 
 phases like the gabbro of Sturgeon Falls, are of eruptive origin. 
 
 1 Geol. Wisconsin, vol. 3, 1873-1879. The Geology of the Menominee Iron Region, Ocorets County, by 
 T. B. Brooks, p. 477. 
 
 2 Ibid., p. 484. 
 
 4 Ibid., p. 518. 
 
 3 Ibid., p. 516. 
 
 fi Gool. Michigan, vol. 4, 1881, p. 209. 
 
WILLIAMS.] 
 
 STURGEON FALLS GABBRO. 
 
 67 
 
 Finally, we may imagine tliat all phases seen at these several places 
 represent material of eruptive origin whose stratiform structure is due 
 to secondary dynamic agencies. This last view has heretofore been 
 advanced only by Irving, who, however, has presented it very briefly, 
 and without descriptions or petrographic proof. 1 
 
 It is the aim of the present portion of this paper to set forth all the 
 evidence that a careful examination of these rocks can furnish as 
 to which of these three views best explains their true origin and mu- 
 tual relations. This material will first be presented in the form of a 
 detailed description of each of the five localities selected for this pur- 
 pose on the Menominee River (see PI. II). The general results thus se- 
 cured will be summarized, in connection with those obtained elsewhere, 
 in Chap. VI. The Menominee localities will be treated of in regular 
 order, commencing with the one farthest down the river, Sturgeon Falls. 
 
 STURGEON FALLS. 
 
 Kinds of rock . — This exposure is situated a short distance below the 
 mouth of the Sturgeon River, in Sec. 27, T. 39 N., R. 29 W., Michigan. Its 
 general topography may be seen from the accompanying map (PI. Ill), 
 which is copied from PI. I, in Major Brooks’s report with double his linear 
 scale. Only the rocks exposed on the eastern or Michigan side of the 
 river were examined ; but those opposite could be seen to be of the 
 same character. 
 
 The barrier which here forms the falls consists of two belts of mas- 
 sive rock, /and h , between which are softer schists, g. These are also 
 intercepted by a harder and more massive band. 
 
 The massive rock is light in color and of a comparatively coarse grain. 
 It is quite elaborately described in Major Brooks’s report, 2 and desig- 
 nated on the authority of Wapler, Rutley, and Pumpelly as a gabbro. 
 Julieu also examined this rock, but. seems to have mistaken the diallage 
 for hornblende, and the brown pleochroic hornblende for biotite. Rut- 
 ley’s opinion is given with hesitation. Pumpelly’s description is brief 
 and accurate. He says : 3 
 
 Saussurite-gabbro (or hornblende gabbro) : contains saussurite, diallage, horn- 
 blende. Identical under the microscope with the coarser crystalline rock of Upper 
 Quinnesec Falls. 
 
 This rock was considered serpentine by Foster and Whitney 4 and 
 was provisionally named ‘‘porpbyritic, speckled diorite” by Brooks, 
 who separated it as his Bed XV of the Huronian. 
 
 The massive occurrence at /is represented by Nos. 11154, 11155, and 
 11162; that at h by Nos. 11107, 11168, 11169, and 11170. Nos. 11156- 
 11161, and 11163-11166 were collected from the softer schistose bauds 
 at g. 
 
 These rocks are particularly noteworthy as being the only ones dis- 
 covered on the Menominee River which contained any trace of pyroxene. 
 
 1 Fifth Annual Report U. S. Geol. Survey, p. 190. 2 Geol. Wisconsin, vol. 3, pp. 455-563. 
 
 Ibid 5 p. 564. 4 Report on the GeoL Lake Superior Land District Plate 2, p. 25. 
 
68 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 | BULL. 62. 
 
 We shall find that they agree perfectly with Pumpelly’s description 
 above cited, the hornblende being in part secondary, and they are hence 
 to be designated as saussurite gabbro. The least altered specimens were 
 found at li (Nos. 11167-11170). The rock at /, although essentially the 
 same as at h , i$ more changed and somewhat schistose along certain 
 bands, while some of the specimens found at g were clearly once the 
 same as the others, but now represent a third and much more advanced 
 stage of alteration. I shall first describe these three stages of the 
 undoubted gabbro, and then trace their relation to the intermediate 
 schists. 
 
 Saussurite- gabbro (first stage ). — The color of this rock in the hand, 
 specimen is rather light. On a fresh fracture it shows a finely mottled 
 structure of white and dark greenish-gray. Examined with a pocket- 
 lens, the mottling is seen to be due to two minerals. One of these is 
 opaque white, sometimes tinged with green, and only rarely exhibits 
 the glistening cleavage surface of feldspar. The darker mineral has a 
 brownish color and almost a metallic luster on its cleavage surface. It 
 is, however, always tinged with green on account of incipient altera- 
 tion. 
 
 No other constituents are microscopically visible. The structure of 
 the rock is irregularly granular. The grain is as a rule moderately fine 
 but is subject to sudden local variation which develops comparatively 
 coarse- grained patches in the main mass. 
 
 Of this freshest type of the gabbro four thin sections were studied, 
 viz, 11167, 11167 a , 11168 and 11170. All show profound alteration in 
 the original constituents, due to dynamic processes. These are, how- 
 ever, most intense in No. 11167, which has been subjected to such great 
 pressure as to present a transition form to the second stage of this 
 gabbro. Nos. 11167 a , 11168, and 11170, are practically identical and 
 may be described together. 
 
 Under the microscope this rock is seen to be composed of plagioclase, 
 almost wholly altered to a gray and opaque saussurite; diallage, of a 
 very light gray color ; hornblende, partly original, partly secondary, and 
 a little titanic iron (hmenite). Certain alteration products, like quartz, 
 caicite, and a colorless chlorite, are also present in varying quantity. 
 
 The feldspar has no crystal form of its own (i. e., it is allotriomor- 
 phous, in the sense of Rosenbusch). It seems to have crystallized sim- 
 ultaneously with the diallage, or if anything later. It is hardly ever 
 so unaltered as to present its original twinning-lamellm, but when this 
 is the case the high extinction angles and brilliant interference colors 
 observed indicate a basic feldspar. No further determinations could be 
 made on this mineral because of its almost complete alteration to a 
 dull opaque white saussurite. Even in the thinnest sections this sub- 
 stance remains opaque for the lower powers of the microscope, being 
 composed of such fine grains that it must be highly magnified before it 
 can be resolved. Under higher powers, however, it is seen to be made 
 
U. S. GEOLOGICAL SURVEV 
 
 BULLETIN NO. 62 PL. Ill 
 
THt l»*kW 
 OF THE 
 
 UHIVERSITT OF U-UHOIS 
 
williams.] ALBITE AND ZOISITE IN SAUSSURITE. 69 
 
 up of small zoisite grains, embedded in a clearer matrix, which is prob- 
 ably albite. 1 
 
 This saussurite substance is traversed in all directions by lighter— 
 sometimes quite clear aud transparent— veins, which are composed 
 largely of secondary albite. This in at least one instance (No. 11168) 
 shows the characteristic twinning striation of plagioclase (see Fig. 4). 
 In other cases, however, these veins appear to be composed of quartz 
 or chlorite (see PI. VIII, fig. 1). 
 
 Fig. 4. — Veins filled with secondary albite in Fig. 5.— Zoisite crystals in a coarse saus- 
 
 the altered gabbro of Sturgeon Falls (Ho. surite from the altered gabbro of Sturgeon 
 
 11168). It.-presented in polarized light in or- Falls. Magnified 180 diameters, 
 
 der to show the twinning striae. Magnified 
 350 diameters. 
 
 In certain cases, notably in section No. 11167, the saussurite aggre- 
 gate is coarser and the zoisite plainly visible aud easily determinable. 
 
 Fig.*5 shows characteristic forms of this mineral. Its crystals are 
 always without terminal planes, but they have a perfectly developed 
 cleavage parallel to their vertical axis and a cross-jointing. Between 
 crossed nicols they are seen to be twinned, sometimes polysynthetically, 
 like albite. The zoisite is itself colorless, with a high index of refrac- 
 tion, but a weak double refraction ; the interference colors are therefore 
 dull, either gray or bluish, and sometimes a deep ultramarine. The ex- 
 tinction is parallel to the cleavage lines. 
 
 One unusually large crystal of zoisite, represented in Fig. 6, exhibits 
 all of these characteristics, and also, when examined in converged polar- 
 ized light, it gives a biaxial interference figure with the plane of the optic 
 axes perpendicular to the cleavage. (Fig. 6.) 
 
 1 Zeitschr. Kryst. u. Min., vol. 7, pp. 234-249. Cathrein, in this article, calculates a number of 
 saussurite analyses to show the relative amounts of feldspar and zoisite or epidote present. He seems 
 to think that the feldspar left after subtracting the zoisite gives the original constitution of the min- 
 eral before its change to saussurite, and attributes the alteration to the addition ofCaO aud A1. 2 0 3 and 
 loss of silica and alkalies (p. 243). Another hypothesis would bo that the original feldspar was much 
 more basic (i. e., contained more CaO, A1 2 0 3 and less §i0 2 and Ha 2 0) than the one now forming the 
 matrix of the saussurite, and that this compound broke up without material chemical change into two 
 compounds, one a more acid plagioclase, like albite or oligoclaso and the other zoisite, which would 
 contain what CaO and superfluous A1 2 0 3 was left after the change. A similar separation of one min- 
 eral into two has boon traced by Profs. J. Brush and E. S. Dana in the alteration of spodumeue into 
 a minute aggregate of eucryptito and albite. (Am. Jour. Sci., 3d series, vol. 20, p. 257 et seq., 1880.) 
 
70 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62- 
 
 The diallage of these rocks is quite colorless when seen in a thin sec- 
 tion, although in the form of powder it is a light grayish green. The 
 prismatic cleavage is well developed, but not as much so as the very 
 perfect parting parallel to the ortkopinacoid, which is the characteris- 
 tic feature of diallage (PI. VIII, fig. 1). The extinction angle was found 
 to be as great as 35° in the prismatic zone. The plane of the optic 
 axes is perpendicular to the orthopinaeoidal parting, and a single axis 
 appears in such sections as show a prismatic angle of nearly 90°. This 
 diallage is very sensitive to the action of pressure and is frequently 
 much bent and twisted. The mineral is sometimes separated along 
 cleavage cracks, the interstices being filled with a colorless, isotropic 
 alteration product, which is probably some variety of chlorite. This 
 substance becomes much more abundant in the more altered forms of 
 this rock and will be again mentioned. The diallage is also often trav- 
 ersed by veins filled with clear quartz. 
 
 Fig. 6. — Large crystal of zoisitein saussurite 
 of No. 11167. Altered gabbro from Sturgeon 
 Falls. Magnified 350 diameters. 
 
 Fig. 7. — Border of both compact and fibrous 
 hornblende around diallage in the Sturgeon 
 Falls gabbro (No. 1167 a ). Magnified 180 diame- 
 ters. 
 
 The hornblende is an important and constant constituent of the 
 Sturgeon Falls gabbro. It is for the most part compact, and brown in 
 color, having the usual pleochroism. More rarely it is green, or ap- 
 parently bleached to a lighter shade of brown. In a few instances 
 this latter process has been carried so far as to make it quite colorless. 
 The hornblende is in all cases most intimately associated with the dial- 
 lage. At times it forms a continuous border of varying width around 
 the diallage crystal, and in other instances it penetrates the latter 
 mineral in irregular areas ( see PI. VIII. fig. 1). In some cases a deli- 
 cate fringe of minute, colorless hornblende fibers is seen to lie on the 
 outer side of the compact hornblende border and penetrate the saus- 
 surite substance (see Fig. 7). This is the same phenomenon that has 
 recently been described by Lossen. 1 
 
 1 Studien an metamorpbischen Eruptiv- uud Sedimentgesteine, etc., cf. Jahrbuch preuss. geol. Land- 
 esanstalt fur, 1884, p. 543, PI. xxix, fig. 2. (Cf. Van Hise: Am. Jour. Sci., 3d series, vol. 33, 1887, pp 
 385 et seq. 
 
WILLIAMS.] 
 
 HORNBLENDE AND CHLORITE IN GABBRO. 
 
 71 
 
 It is impossible to say with certainty what the origin of the com- 
 pact brown hornblende is. It may be an original product of crystal- 
 lization in the magma, but its mode of occurrence and its general 
 character indicate that it is probably of secondary origin, having 
 originated by paramorphism of the diallage, as has been shown by my- 
 self 1 and by Lossen 2 to be sometimes the case. 
 
 No other constituents are important in this rock. Iron in any form 
 seems to be quite rare in it. Occasional cloudy grains, resembling 
 leucoxene, may represent some original ilmenite, while minute crystals 
 of pyrite are still rarer. 
 
 The structure of the rock seems to be irregularly granular ; none of 
 the components being in any degree idiomorphic. Frequent and 
 abrupt changes in the coarseness of the grain are observable. 
 
 All specimens show the action of dynamic forces which have more or 
 less profoundly affected the different constituents. These effects are 
 particularly noticeable in slide No. 11167. Here the rock seems in 
 places to have been crushed and a mosaic of the component minerals 
 to have been formed. Hornblende, generally colorless, is unusually 
 abundant. Colorless chlorite and zoisite are also developed, and all are 
 mixed indiscriminately. In one part of the section a vein is s* en to 
 traverse the rock. This is filled with limpid quartz in long, wedge- 
 shaped areas, which extend from one side of the small fissure to the 
 other. This quartz is traversed by 
 long, colorless fibers of the greatest 
 delicacy, and it also contains a good 
 deal of the colorless chlorite, both in 
 solid masses and in those peculiar 
 vermicular groups to which Volger 
 has given the name helminth. These 
 curious groups, which resemble piles 
 of little coins, are sometimes straight, 
 sometimes curved. They are so mi- 
 nute as to be visible only with a high 
 magnifying power. Fig. 8 represents 
 them as they appear when magnified 
 350 diameters. Exactly the same min- 
 eral has been described in the sec- 
 ondary quartz of diabase by Molil, 3 von Lasaulx 
 in that of schalstein and syenite by Hussak. 6 
 
 Samsurite gabbro [second stage ). — Representatives of this type are 
 found at the lower end of the falls, at / on Major Brooks’s map, and 
 
 'Am. Jour. Sci. 3d series, vol. 28, Oct., 1884, p. 262. 
 
 2 cf. J ahrbuch preass. geol. Landesanstalt fur 1883, p. 632. 
 
 3 if cues J ahrbuch fur Mineral., 1875, p. 716. 
 
 4 Verh. d. naturh. Vereins d. preuss Rlieinl. u. Westf., 1878, p. 216. 
 
 6 Inaugural-Disseitation. Bonn, 1884, p. 22. 
 
 6 Tschermak’s mineral, u. potrog. Mittheil., vol. 1, 1878, p. 275. 
 
 Pig. 8. — Vermicular chlorite (helminth) in 
 quartz. Vein in altered gabbro, Sturgeon 
 Palls. 
 
 and Schenck f and 
 
72 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL * 62 . 
 
 at his e , at the lower end of the basin below the falls. Nos. 11153 and 
 11154, from these two localities, are identical in mineral composition 
 with the rocks of the first type above described. They are of a dirty 
 greenish gray color and indications of a schistose structure have already 
 begun to appear in them. Under the microscope they disclose the 
 same constituent minerals as the rocks of the first type; nor are these 
 minerals much more altered, but they show the effects of a profound 
 mechanical action. The feldspar is remarkably fresh and its twinning 
 lamellse are quite distinct, but it is everywhere crushed, broken, and 
 faulted. The crystals are often plainly seen to be separated into a 
 number of fragments which are removed a considerable distance from 
 one another. Frequently a fine grained mosaic has been formed by 
 the crushing of the larger feldspar crystals. In other cases (especially 
 in section 11154) the feldspar is not so much broken, but it is altered 
 around its edge to an opaque, gray saussuritic mass, while its interior is 
 hardly changed. (See PI. VIII, fig. 2). The diallage is more altered 
 than in the rocks last described, although it can still be seen to belong 
 to the same species. The crystals are very much bent and twisted and 
 frequently so changed to the light-colored chlorite that only a few 
 minute remnants of the brightly polarizing mineral remain m this 
 nearly isotropic base. (See PI. VIII, fig. 2.) Fibrous hornblende now 
 becomes more abundant than the compact, and leucoxene patches are 
 seen at intervals. 
 
 Nos. 11162, from the upper part of the point /, and 11172 from above 
 the falls at n , present interesting varieties of this rock. They do not 
 show the effects of crushing to such a degree as do those just described. 
 Indeed the original structure of the rock seems well preserved, although 
 the feldspar is almost completely changed to a fine grained, nearly 
 opaque saussurite, and every trace of the pyroxene (diallage) has dis- 
 appeared. A pale green, fibrous hornblende occupies the place of this 
 mineral, and there seems to be every reason for regarding it as derived 
 from the diallage ; although in No. 11172 the abundant remains of a 
 compact, brown hornblende, evidently in the process of changing to 
 the fibrous modification, suggests the possibility of this mineral having 
 been the original bisilicate constituent. Still there is no warrant for 
 assuming that what is essentially a diallage rockmass was locally de- 
 veloped as a hornblendic rock ; and it may be that this is an instance 
 of a remarkable passage of a pyroxene through a compact into a fibrous 
 hornblende , for which we shall find much evidence in the studies that 
 follow. 
 
 Saussurite gabbro ( third stage). — As has been already remarked and as 
 may be seen on the map of Sturgeon Falls (PI. Ill), there is, between 
 the two points of the more massive rock, li and /, an area </, composed 
 of softer schists. These are easily eroded and have thus occasioned the 
 small bay. The passage from the fresh and massive gabbro at h into 
 
WILLIAMS. ] 
 
 EXTREMELY ALTERED GABBRO. 
 
 73 
 
 these schists seems to be a gradual one. Aloug the lower side of h 
 there are rocks which are without doubt essentially the same as those 
 above described from this point but which have been profoundly altered 
 by dynamic action, which has also occasioned considerable chemical 
 changes. These rocks, while they show remains ot their original min- 
 erals, have become decidedly schistose ; and by the alteration in their 
 composition, they have developed certain other points of similarity 
 with the schists at g , into which they appear gradually to pass. For 
 this reason they have been selected to represent the third and most 
 altered stage of the gabbro in which any sure signs of the original 
 character of the rock still remain ; at the same time they possess even 
 more of the characters belonging to the schists, and thus afford just 
 the evidence desired that the latter are the extremely modified form of 
 the massive rock. 
 
 No. 11166 is only indistinctly schistose, showing a soft grayish green 
 matrix in which are imbedded altered grains of a reddish feldspar. 
 Under the microscope the original coarsely granular structure of the 
 rock may still be made out. Large but much broken areas of feldspar 
 may be clearly seen where but very little of the unaltered substance 
 remains. For the most part this has been changed to an aggregate of 
 calcite and minute, brightly polarizing needles or plates of a colorless 
 micaceous mineral (probably sericite) aloug with occasional areas of 
 secondary quartz. What was once the pyroxene or hornblende is now 
 a colorless or extremely pale green, scaly mineral which an examination 
 shows to be chlorite. Between crossed nicols it is isotropic or very 
 feebly polarizing. It was separated by the Thoulet solution from the 
 slightly heavier feldspar and as a powder appears pale green. In a 
 closed tube it gives off water abundantly and becomes dark. With hot 
 sulphuric acid it decomposes and gelatinizes immediately ; with hydro- 
 chloric acid it decomposes slowly, givinga somewhat yellowish solution, 
 from which ammonium-hydroxide precipitates alumina abundantly. 
 There can therefore be no doubt that this mineral is a chlorite very poor 
 in iron, like the nearly colorless pyroxene from which it is derived. 
 Areas of leucoxene are also common through this rock. 
 
 No. 11165, taken from a place only a foot or two below the last and 
 undoubtedly continuous with it, is decidedly more schistose. Under 
 the microscope the minerals are essentially the same as in the last 
 specimen, but the mechanical effects here exhibited are much more 
 intense. The feldspar and the diallage are still recognizable, but the 
 colorless chlorite is much more abundant than in any specimen before 
 described. The feldspar areas have a brownish color, even in the thin 
 section and they are pulled and torn asunder in a remarkable man- 
 ner. Individuals are often pulled out into more than twice their orig- 
 inal length, the separation taking place along a series of interlacing 
 cracks which run approximately perpendicular to the schistose structure 
 
74 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62 . 
 
 of the rock. The spaces between the separated fragments are filled 
 with the chloritic mineral. This rock shows every indication of having 
 been enormously stretched and this process, along with attendant 
 chemical changes, has induced its schistose structure. Although it 
 shows under the microscope traces of the original gabbro structure and 
 of the original gabbro minerals, no one would hesitate from a micro- 
 scopical examination to class it with the schists. 
 
 The schists above mentioned as occurring between the two masses 
 of typical gabbro, li and /, at the Sturgeon Falls, possess an important 
 relationship to these rocks. Taken by themselves, they offer as rep- 
 resentative examples of fissile, silky, hydro- mica or sericite schists as 
 could anywhere be found, and yet this narrow band presents such a 
 complete series of transition forms that their origin as derivatives of 
 the massive rock cannot be doubted. In fact, two such series were 
 traced out in detail. One of these was collected on the lower side of 
 h and represents the passage of the least altered and most massive 
 gabbro into the typical schist, and the other was obtained near the 
 center of the schist band where a narrow strip of the rock has hap- 
 pily been preserved from the extremest alteration and plainly 
 shows its identity with the gabbro proper. This narrow layer, rep- 
 resented on the map at g , is of great value in conclusively proving the 
 origin of the schists in the midst of which it lies and into which it 
 passes on both sides. 
 
 No. 11160, from this locality ( g ), was classified in the field-notes with 
 the schists, and regarded as only a harder and more slaty form of these. 
 Indeed, this rock is very schistose, cleaving readily in a direction par- 
 allel to the foliation of the more fissile schists. Under the microscope, 
 however, an original gabbro structure is still distinctly seen. Triclinic 
 feldspar, in broken and bent crystals, is plainly visible, while the other 
 constituents have passed into colorless chlorite, quartz and calcite. 
 The feldspar itself is mostly altered into the same compounds, though 
 its form and occasionally its twinning striae are still preserved. 
 
 No. 11161 is a hard, greenish slate, occurring beside the last described 
 rock. Under the microscope, in ordinary light, crystal forms are seen 
 outlined in a dark color, the matrix being colorless. In polarized light, 
 however, these are no longer visible, and there is only a fine grained 
 and schistose aggregate of colorless chlorite, quartz and calcite. 
 
 Nos. 11159 and 11158, collected just below the last, are typical schists 
 of a light gray color and somewhat greasy feel. They contain just the 
 same minerals as the rocks last described, but here every trace of orig- 
 inal structure has disappeared. There is no indication of the form of 
 any earlier constituents, but those now present are arranged in a finely 
 parallel mosaic of somewhat varying grain. Calcite is much more 
 abundant than in the previous instances. Indeed, in No. 11158 this 
 mineral makes up a large share of the rock. 
 
 The other series of transition forms between the gabbro and the 
 
WILLIAMS. J 
 
 SCHISTS DERIVED FROM THE GABBRO. 
 
 75 
 
 schists occurs on the lower side of the gabbro mass h. This series em- 
 braces the specimens of the first, second, and third stages of the gabbro 
 already described from this exposure, and terminates with two speci- 
 mens of schist, Nos. 11163 and 11164. Any sharp line of demarkation 
 between the typical and massive saussnrite-gabbroat /*, and the fissile, 
 silvery schists, apparently so different, lying below it, was sought long 
 and carefully, but in vain. In fact no such line exists, and if one were 
 to be drawn it must be drawn arbitrarily. The rocks already described 
 from this locality as specimens of the gabbro in the third stage show 
 this. No. 11165 is entered in the field-notes as belonging to the 
 schists, but microscopical examination shows it to be even more closely 
 allied than the almost massive No. 11166, to the gabbro. Traces of the 
 original components and structure are by no means rarest in those 
 rocks which appear macroscopically to have suffered the most profound 
 alteration. 
 
 Nos. 11164 and 11163 are light gray, silvery schists, with a somewhat 
 greasy feel; such in fact as might ordinarily be classed as sericite or 
 hydro-mica, schists. Their lamination, however, is not in the least regu- 
 lar, but undularory, aud there is a tendency to cleavage not so much 
 along a single plane as in almost any plane parallel to a line. In other 
 words, these rocks have a well marked dip, but hardly any determina- 
 ble strike. In 11164 especially, there is noticeable a jointing trans- 
 verse to the strike, and these joint planes often gap open into wide, len- 
 ticular seams, as though the rock had been stretched in the direction 
 of its strike. 
 
 Under the microscope these rocks are seen to be mostly composed of 
 the nearly colorless chlorite, calcite, and a little secondary quartz. 
 These minerals are interlaced in narrow, wavy bands, producing what 
 may be called after the German idiom, a long “ micro flaser v structure. 
 But even here every trace of the original constituents has not yet dis- 
 appeared. Occasional battered and broken feldspar remnants are en- 
 countered, with their fragments widely separated, and for the most part 
 changed to sericite or calcite. Around these curve and twist the silky 
 chlorite bands developing a sort of “Augen” structure, which may be 
 best seen by examining a section with an ordinary pocket lens. The 
 areas of leucoxene also, before observed, are not lacking here, but 
 these are pulled out in the direction of the schistose structure, un- 
 til a single one may be followed nearly across an entire section. The 
 bisilicates have evidently all passed into the colorless chlorite, aud this 
 mineral on account of its pliability has easily accommodated itself to 
 the circumstances, and has developed the pronounced schistose struct- 
 ure which is now the most important feature of the rock. 
 
 These rocks are schists, indeed, of the most characteristic type, but 
 in the light of their field relations and still more from the evidence 
 which a microscopical study of the whole series has afforded, it is evi- 
 dent that they represent the most altered form of the massive gabbro, 
 between two areas of which they are included. 
 
76 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 Chemical analyses.— In order to ascertain what changes have taken 
 place in the chemical composition of the Sturgeon Falls gabbro during 
 the process of its alteration into the schists, the following analyses of 
 specimens illustrating three successive stages of the alteration were 
 made by Mr. E. B. Eiggs : 
 
 
 I. 
 
 II. 
 
 III. 
 
 Si0 2 
 
 51.46 
 
 38.05 
 
 45. 70 
 
 A 1203 
 
 14. 35 
 
 24. 73 
 
 16. 53 
 
 Fe 2 o 3 
 
 3. 90 
 
 5. 65 
 
 4. 63 
 
 FeO 
 
 5. 28 
 
 6. 08 
 
 3. 89 
 
 CaO 
 
 9.08 
 
 1.25 
 
 4. 28 
 
 MgO 
 
 9. 54 
 
 11.58 
 
 9. 57 
 
 XajO 
 
 2. 92 
 
 2. 54 
 
 .55 
 
 K 2 0 
 
 .24 
 
 1.94 
 
 3.82 
 
 H 2 0 
 
 3.30 
 
 7.53 
 
 4. 70 
 
 C0 2 
 
 .20 
 
 .93 
 
 5. 95 
 
 Total 
 
 100. 27 
 
 100. 28 
 
 99. 62 
 
 Rock powder dried at 105° C. 
 
 I. No. 11170, freshest gabbro from the point h. 
 
 II. No. 11166, gabbro in third stage from the south side of li. 
 
 Iir. No. 11164, silvery schist from between g and h. 
 
 At first glance these analyses seem to present a curious anomaly. 
 The intermediate rock, No. 11 166, appears to differ more from the orig- 
 inal type than the most altered specimen, No. 11164. A closer exam- 
 ination, however, shows that the nature of the chemical processes which 
 have gone on in the two cases is essentially different. In the first case, 
 No. 11166, this has been chiefly chloritization, while in the second case, 
 No. 11164, the chloritization has been less, but sericitization and car- 
 bonatization have also been extensive. 
 
 The abundance of the colorless chlorite, above described as present 
 in No. 11166, here manifests itself in the very low percentage of silica 
 and in the correspondingly high percentage of alumina, together with 
 the increase of both magnesia and water. The iron is unusually low 
 in this chlorite because it did not exist in the mother rock; still there 
 has been a gain rather than a loss of this ingredient. The lime has 
 here been to a great extent removed, presumably in the form of the 
 soluble bicarbonate, while the slight sericitization, above mentioned in 
 the description of this rock, is indicated by the increase of the potash. 
 
 In the analysis of No. 11164, the less extent of the chloritization is 
 shown by the less, although proportionate, increase of alumina and 
 water and decrease of silica, while the iron and magnesia remain about 
 the same as in the mother rock. Here the lime has been partly, re- 
 moved as before and partly retained as calcite, visible everywhere 
 through the Tock and indicated in the analysis by the 5.95 per cent of 
 C(J 2 . The sericitization, so apparent under the microscope, is here 
 shown by the great increase in potash and the exchange of the soda 
 for potash. 
 
WILLIAMS.] 
 
 LOWER QUINNESEC GREENSTONE. 
 
 77 
 
 LOWER OR LITTLE QUINNESEC FALLS. 
 
 The rock exposure of Lower Quinnesec Falls is not confined to the 
 immediate vicinity of the falls but it extends, especially on the left 
 bank of the river, for a considerable distance below. This portion 
 forms a high, abrupt and homogeneous ridge, of uniform composition 
 and structure, the description of which may be advantageously sepa- 
 rated from that of the rocks occurring immediately at the falls. 
 
 We shall, therefore, consider under two successive heads: 
 
 (Id The greenstones of the so-called “ Gabbro Ridge” of Major Brooks. 
 
 (2) The greenstones of the Lower Quinnesec Falls. 
 
 Greenstones of the so-called “ Gabbro Ridge” of Major Broolcs . — For a 
 mile below Lower Quinnesec Falls, the north bank of the river is skirted 
 by an almost perpendicular wall of massive greenstone. This wall is 
 sometimes over a hundred feet in height, and has every appearance of 
 being a great dike. Although for the most part it is quite massive, it 
 presents frequent and very instructive evidence of the effect of great 
 pressure upon it. It is seamed and gashed, broken and torn, and con- 
 tains schistose bands of varying width. Since the continuity of these 
 bands with the massive rock is established, their study is calculated 
 to throw light on the subject of dynamical metamorphism. 
 
 Major Brooks designated the rock which composes this ridge as a 
 “massive gabbro,” aud correlated it with the above-described saussu- 
 rite-gabbro of Sturgeon Falls. My studies have, however, failed to 
 disclose in this rock any trace of pyroxene. In addition to its feld- 
 spathic constituent, which is generally altered to saussurite, it contains 
 in abundance that peculiar pale green and more or less fibrous variety 
 of hornblende which is quite universally conceded to be of secondary ori- 
 gin. What the primary form of all this green hornblende was, it is now 
 impossible to ascertain with certainty. It is of a kind well known to 
 originate from the alteration of pyroxene. The rock as a whole also 
 bears decidedly the character of a diabase or pyroxene rock; and yet, 
 not a trace of pyroxene has been discovered in any of the Menominee 
 River greenstones, if we except the light colored diallage of the Stur- 
 geon Falls gabbro. Whenever the pale green hornblende can be traced 
 back to an original form, it is seen to be derived from a compact 
 brown or basaltic hornblende. This fact was substantiated not merely 
 for the rock composing the ridge here under discussion, but it is also 
 true foi the several other localities examined on the river. 
 
 This brown hornblende is seen first to turn green by a reduction of 
 its iron to the ferrous state, or to become bleached by loss of its iron, 
 and finally to break up into an aggregate of fine hornblende needles 
 exactly similar to that commonly formed by the alteration of pyroxene 
 to uralie. 
 
 It is, of course, impossible to prove that some of the secondary fibrous 
 hornblende has not been derived from pyroxene. Indeed, it seems very 
 probable that both augifce and compact, brown hornblende may have 
 
78 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BIH.L. 62. 
 
 existed side by side as original constituents of the rock, and that both 
 finally succumbed to the same process of alteration, although the horn- 
 blende resisted this much longer than the augite. Such, in point of 
 fact, has elsewhere been observed to be the case where both minerals 
 have undergone uralitization in the same rock; 1 and this would account 
 for the frequent survival of brown hornblende cores where every trace 
 of pyroxene had disappeared. 
 
 If this is not the true explanation of the genesis of these rocks, there 
 are but two other hypotheses possible — either that the original rock 
 contained no pyroxene, but was a diorite, composed of plagioclase and 
 brown hornblende ; or, that the pyroxene has passed into uralite through 
 an intermediate compact, brown hornblende. Opposed to the first of 
 these suppositions is the structure of the rock, which is diabasic rather 
 than dioritic. On the other hand, considerable evidence afforded by 
 various of the Menominee rocks, as well as observations made elsewhere 
 by the writer 2 and by Lossen, 3 indicate that the latter hypothesis may 
 possibly be true. Inasmuch, however, as the rocks here under discuss- 
 ion afford no trace of pyroxene, it hardly seems justifiable to call them 
 anything but diorite. We shall encounter still more distinct examples 
 of this type farther up the river. 
 
 All the specimens collected from this greenstone ridge show an 
 advanced stage of alteration. Some obtained from the western ex- 
 tremity of the ridge, near the Michigan bank of Lower Quinnesec 
 Falls, have a coarsely porphyritic structure, and are among the freshest 
 specimens that were procured. This variety of the rock is represented 
 by Nos. 11034, 11035, and 11098. Of these the last is perhaps the most 
 typical. To the unaided eye it shows a light greenish gray matrix, 
 thickly studded with irregularly shaped crystals of opaque white feld- 
 spar (saussurite) from one-halt centimeter to two centimeters in diame- 
 ter. A closer examination reveals many brightly reflecting cleavage 
 surfaces of another and darker mineral. These are of about the same 
 size as the feldspar crystals, but their continuity is interrupted by small 
 opaque spots, which produce the mottled structure recently termed by 
 the writer pcecilitic . 4 The color of these cleavage surfaces, which with 
 the aid^of the microscope are found to belong to large individuals of a 
 somewhat altered hornblende, is so nearly like that of the ground mass 
 of the rock that unless their reflection is caught in just the right light 
 they escape detection. 
 
 The large porphyritic crystals of feldspar are almost wholly changed 
 to saussurite. This has a dull gray color, and is nearly opaque even in 
 the thinnest sections. A high magnifying power resolves it into an ag- 
 gregateof minute zoisite needles. Curiously enough, these feldspar crys- 
 tals show a clear zone of unaltered substance around their outer edge. 
 
 1 Bull. U. S. Geol. Survey, No. 28, p. 45. 
 
 2 Ara. Jour. Sci., 3d series, vol. 28, p. 262, Oct., 1884. 
 
 3 Jahrbuch preuss. geol. Landesanstalt fur 1883, p. 632, Berlin, 1885. 
 
 4 From 7roifciAo9, mottled. See Am. Jour. Sci., 3d series 1886, vol. 31, p. 30. 
 
WILLIAMS.] 
 
 ALTERATION OF THE HORNBLENDE. 
 
 79 
 
 This fresh and finely striated portion presents a striking contrast to the 
 dull gray saussurite, and it is difficult to imagine how it has so com- 
 pletely escaped the alteration which has attacked the rest of the crys- 
 tal, unless it is the product of a more recent growth. 
 
 With the exception of groups of ilmenite grains, which are beauti- 
 fully fringed with a leucoxene border, the remainder of this rock is com- 
 posed almost wholly of hornblende. In its freshest state this mineral 
 has a compact structure and coffee brown color, with the usual pleO- 
 chroism and other optical properties of the species. Its first phase of 
 alteration consists in turning green, and this is followed by a gradual 
 bleaching. This process continues until the mineral has become quite 
 colorless, without, however, losing its compact structure. In the larger 
 individuals of compact hornblende, whether this is brown, green, or color- 
 less, occur numerous small lath-shaped feldspars, which produce the 
 mottled or “pcecilitic” structure above alluded to. These seem to be 
 less completely changed to saussurite than the larger feldspar crystals, 
 but they often contain the zoisite crystals in a more perfect state of 
 development. 
 
 It has already been mentioned that 
 these hornblende crystals show an 
 advanced stage of alteration. The 
 hornblende itself is bleached until it 
 is nearly colorless. The final change 
 seems to be the breaking up of this 
 bleached hornblende into an aggre- 
 gate of colorless needles, resembling 
 tremolite. In other cases, however, 
 it is changed in irregular patches to 
 a colorless chlorite which is quite 
 isotropic, and only visible between 
 crossed nicol prisms. The peculiar 
 manner in which this takes place de- 
 serves particular notice, and is repre- 
 sented in Fig. 9. The hornblende 
 substance remains in interlacing veins between the chlorite areas. 
 It is brightly polarizing and may be often seen, as in the figure, to 
 be continuous with an unchanged hornblende individual. This peculiar 
 mode of alteration is doubtless also conducive of the “ pcecilitic” effect 
 above mentioned. The clearness, transparency, refraction, etc., of both 
 hornblende and chlorite are so nearly identical that this structure is 
 wholly invisible in ordinary light, and the effect of polarized light in 
 transforming the apparently homogeneous and colorless mass into its 
 two strongly contrasted elements is very striking. 
 
 No. 11034 is essentially the same as the specimen just described, 
 except perhaps that it is more altered, and hence contains less of the 
 original compact brown hornblende. Most of the hornblende, indeed, 
 
80 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62 . 
 
 in this rock is colorless, and much of it is fibrous. That which still 
 retains any color is for the most part green. 
 
 No. 11035 was not sectioned, but in the hand-specimen it exactly 
 resembles the others. 
 
 No. 11032, collected with the specimens last described, is a beautiful, 
 fresh looking rock, without porphyri tic structure, but with its hornblende 
 in long, slender, greenish-black crystals. Under the microscope the 
 feldspar of this rock is seen to be less altered than in those above 
 described. Saussurite is abundantly developed in it, but not so exten- 
 sively as in the porphyritic crystals of the other specimens. There is, 
 however, here no brown hornblende. This mineral is all of a pale green 
 color, or it is changed to chlorite, which sometimes contains sharp 
 crystals of epidote. Ilmenite is abundant and is fringed with leu- 
 coxene. 
 
 The above described specimens, from the extreme western edge of 
 the ridge near the falls, although they are the least altered form of the 
 rock, hardly represent its most typical aspect, as the ridge is followed 
 along the river bank, westward from Sandy Portage, its high and almost 
 perpendicular front is found to be composed of a light green or grayish- 
 green, fine grained or aphanitic rock. This is compact and massive in 
 structure, but everywhere profoundly seamed and jointed. It is cut by 
 cross-gashes aud parted joints, and gives every indication of having 
 been pulled or crushed — at all events, of having been subjected to 
 enormous mechanical strains. The joints and seams often run in many 
 different directions, producing a regular breccia without cement. The 
 rock is also much slickensided, frequently so much so as to produce a 
 schistose structure. The layers thus formed sometimes bend around 
 more massive cores, which seem to have resisted the rubbing action. 
 
 The formation of what are above described as “cross-gashes” is 
 very curious. At times the entire face of the rock wall is scarred with 
 approximately parallel gaping seams, closely resembling the rents formed 
 in moderately dry clay or putty when this is stretched. A single open- 
 ing does not extend for any great distance, but a great number of them 
 of all dimensions, closely crowded together, may produce an irregular 
 sort of foliation. The general appearance of a rock thus gashed is rep- 
 resented in Fig. 10, which was drawn from a hand-specimen. This of 
 course can give only an approximate idea of the appearance of this 
 structure in a large rock-mass. These gashes seem to have been pro- 
 duced by a stretching of the rock, or, what amounts to the same thing, 
 by a bulging perpendicular to the action of some great pressure. They 
 r esemble the “ Idaffende Bisse described by Heim in the Alps, and al- 
 ready mentioned in Chapter I ( p. 43). The edges of the seams are ragged 
 as though they had been formed by a forcible tearing asunder of the 
 rock after it was solid. They are often filled with subsequent infiltra- 
 tions of secondary minerals, like calcite or quartz, but more frequently 
 they are open. 
 
STRETCHED GREENSTONE. 
 
 81 
 
 WILLIAMS. J 
 
 No. 11028 is a fair average specimen of the rock composing this ridge. 
 It is a grayish green, compact, homogeneous mass, which is but little 
 
 jointed. Under the microscope it is seen to be mainly composed of a 
 
 1 ‘ 
 
 Fig. 10.— “ Cross-gashes” in a greenstone from Lower Quinnesec Falls. 
 
 finely fibrous, pale green hornblende of secondary origin, of saussurite, 
 quartz, and ilmenite. The structure of the rock has been almost en- 
 tirely destroyed in the course of the mineralogical changes which have 
 taken place in it. As the new minerals have formed they have wan- 
 dered from the position occupied by the older ones and have thus pro- 
 duced a fine grained and confused aggregate in which remains of larger 
 rectangular feldspars or hornblende crystals are only rarely discernible. 
 The ilmenite is scattered about in minute dots, each surrounded by its 
 own leucoxene border. The quartz is in irregular patches and bears 
 every evidence of being secondary in its origin. 
 
 No. 11033, from near the western end of the ridge, is almost identical 
 with the specimen last described, but contains more quartz, and the 
 remains of the feldspar imbedded in a dark gray, opaque matrix. 
 
 No. 11031 is a specimen collected from very near the spot where No. 
 11028 was obtained, and the two, when taken in connection, show in a 
 very clear and beautiful manner the effect of mechanical action in modi- 
 fying both the macro-structure and the micro-structure of a solid rock. 
 
 Bull. 02 0 
 
82 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 . 
 
 In spite of great present differences, there can be no doubt that the 
 two specimens were once portions of a continuous mass. They were 
 taken side by side from a single ledge which showed nothing like a line 
 of contact between two different rocks. One is a typical massive green- 
 stone, with hardly a joint-plane visible in it; the other, while agreeing 
 closely with the first in color and texture, is deeply cracked, gashed 
 and seamed, and possesses a pronounced schistose structure. The orig- 
 inal form of both specimens was doubtless an igneous rock of the dia- 
 base type, which has been subjected in one case (Ho. 11028) to chemical 
 (metasomatic) and in the other (Ho. 11031) to dynamic metamorphism. 
 
 Rocks may be altered by simple pressure, but the accumulated strains 
 which are generated within them are relieved and adjusted by over- 
 coming the force of cohesion along certain planes. Here there will be 
 a shearing motion of greater or less extent, and a consequent crushing 
 of the rock. The rent is soon healed by the crystallization of new com- 
 pounds which cement the crushed fragments, and in this way a schistose 
 band, of width varying with the intensity of the force, may be devel- 
 oped in the midst of an otherwise solid and massive rock ; or a number 
 of such bands may be formed parallel to one another, and together im- 
 parting to the rock the appearance of a foliated or even a banded 
 schist. 
 
 Conclusive proof of this process might be difficult to discover without 
 the aid of the microscope, but this instrument is happily able to afford 
 sufficient evidence to overcome all doubt. We shall have many instances 
 of such action to describe in the sequel, each of which will exemplify 
 some particular phase of the process. 
 
 The two rocks here under discussion, however, illustrate this general 
 principle in an admirable manner. Plate IX represents the appearance 
 of each of them in a thin section as seen under the microscope. The 
 structure of the first, Ho. 11028, is, as above described, a granular aggre- 
 gate of fibrous hornblende, chlorite saussuritized feldspar, quartz, and 
 ilmenite, produced by chemical action alone in recrystallizing the ele- 
 ments of the original constituents in new compounds more in accord- 
 ance with the altered physical conditions to which the rock was sub- 
 jected. The component minerals of the second rock (Ho. 11031) are 
 not so different from the last, but the story of its origin is told in its 
 structure. The primary constituents seem to have been literally pul- 
 verized by crushing. The feldspar crystals have been pulled apart, 
 the fragments being separated a considerable distance (always, how- 
 ever, in the same direction), but it is still possible to recognize frag- 
 ments which once belonged together. The substance of this feldspar 
 is remarkably fresh, another instance of the chemical action which takes 
 place in this mineral being inversely proportional to the mechanical 
 action which has affected it. The separation of the feldspar fragments 
 is due to a stretching action and the spaces between them are filled 
 with a pale green and almost isotropic chlorite. This mineral has 
 
williams.] PROCESS OF ALTERATION IN THE GREENSTONES. 
 
 83 
 
 evidently been developed at the expense of the hornblende, which is 
 here only rarely to be found, and then always in bauds where the me- 
 chanical deformation has been less intense. Where it is found, how- 
 ever, this hornblende is identical with that occurring in No. 11028. The 
 ilmenite and leucoxene are seen as before, but the former is far less 
 abundant while the latter is proportionately more abundant. When 
 the ilmenite has completely disappeared, the leucoxene forms bands and 
 stringers, thus aiding in the production of a schistose structure. 
 
 This development of chlorite out of the hornblende substance seems 
 to be a very important feature in the stretched basic eruptive rocks 
 and many other instructive examples of it will be given beyond. It 
 has a definite bearing upon the origin of the fine grained chlorite schists 
 which accompany and are interstratified with so many of them. 
 
 Nos. 11041 and 11042 form an instructive pair of specimens, collected 
 near' the river bank toward the western end of the ridge. At this 
 particular locality there is a well marked band of green schist travers- 
 ing the here generally massive greenstone in a direction 8. 70° E. The 
 schistose structure is irregular and undulatory, and on either side there 
 is a gradual passage from the schist into the massive rock. No. 11042 
 is from the surrounding mass immediately at the edge of the schist 
 band. In a hand- specimen it appears to be considerably altered, of a 
 gray color, and without any cleavage. Under the microscope the orig- 
 inal structure i& easily recognizable. The rock is largely composed of 
 stout rectangular feldspars, with a somewhat rounded outline, and in- 
 ternally changed to saussurite, though their periphery is mostly clear. 
 Between these are the remains of former hornblende (possibly pyroxene) 
 individuals now represented only by amphibole fibers and chlorite. 
 Beautiful skeleton forms of leucoxene, composed of three sets of par- 
 allel bands, reproducing the rhombohedral parting of the original ilrneu- 
 ite, are abundant. 
 
 No. 11041 is the same rock as the last in a much more altered form. 
 The feldspar is mostly changed to calcite, and the hornblende to chlo- 
 rite. The structure has wholly disappeared and there is a very fine mo- 
 saic of quartz and secondary albite substance. Still, the same skeleton 
 forms of leucoxene remain and there is no doubt that the two speci- 
 mens represent the same rock in different stages of alteration, the 
 more changed form having become decidedly schistose. 
 
 Farther west, in the immediate vicinity of Lower Quinnesec Falls, the 
 abrupt face of the diorite ridge proper retires a short distance from the 
 river bank. Along the shore the massive greenstones give place to slaty 
 rocks, which cleave into rhomboidal prisms. They have no proper strike, 
 but seem to break with equal readiness in all planes parallel to a line; 
 and this line is here nearly perpendicular 4o the surface. No. 11043 is 
 one of these rocks of a greenish color. Under the microscope it is seen 
 to have been so profoundly altered that it is now impossible to assert 
 from internal evidence what its original character was. Still, its geo- 
 
84 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 logical position indicates that it was once a part of thegabbro or diorite 
 ridge, and there is nothing in its present structure that directly contra- 
 dicts this supposition. The rock has a pronounced, although irregular 
 and undulatory, schistose structure. It consists largely of a fine grained 
 matrix, composed of chlorite scales, arranged parallel to the direction 
 of schistosity. With this mineral are associated quartz, feldspar, opaque 
 black grains, probably magnetite, and occasionally sharply defined crys- 
 tals of muscovite. Imbedded in this groundmass are larger feldspars, 
 sometimes in well developed crystals, sometimes in fragments. The 
 substance of these is but very Tittle altered, and yet their outline is 
 made indistinct by. the penetration into them of the chlorite scales. 
 They often appear to have been much squeezed and broken, the frag- 
 ments being more or less separated. Grains of quartz are occasionally 
 seen, which have also been fractured by pressure. Calcite, due to 
 alteration, is also sparingly present. 
 
 Similar rocks, more or less schistose and varying from a dark green 
 to a light gray, occur from this point along the river bank all the way 
 to the falls. 
 
 No. 1104G is from the light silvery-gray, greasy-feeling baud, which 
 projects into the basin at the foot of the falls. This is a typical sericite 
 schist. Under the microscope it is seen to have a finely schistose struct- 
 ure, produced by the parallel arrangement (often in bands) of quartz 
 grains, sericite scales, and chlorite, which is nearly colorless. Along 
 with this is a large amount of calcite, also distributed in bands. There 
 is no feldspar visible. The most interesting constituent is rutile. This 
 mineral is sparingly distributed through the whole rock in very minute 
 and sharply defined crystals. These have a pale yellow color, a high 
 index of refraction, and the usual twinned forms. In certain portions 
 of the section there are dull gray, opaque spots, which are yellow in 
 reflected light. These are not continuous, but are more or less broken 
 up and pulled out in the direction of the schistose structure. They 
 contain occasional dark red and irregularly shaped graius of rutile, but 
 for the most part they are composed of innumerable small rutile needles 
 (quite like the u Thonschiefernadeln v of the Germans) so closely crowded 
 together as to form an opaque mass, only resolvable with a high power 
 of the microscope. From these dense masses the other little needles 
 in the other parts of the rock seem to have wandered. 
 
 This rock is almost identical with certain light colored, very fissile 
 schists occurring on the opposite side of the river (cf. No. 11011, de- 
 scribed beyond), and the strike of these two exposures seems to identify 
 them as belonging to a single band. 
 
 Greenstones of the Lower QiUnnesec Falls . — Passing now to the rocks 
 exposed along the northern or northwestern shore of the basin below 
 Lower Quinnesec Falls, we find alternating bands of lighter and darker 
 colored greenstones, each accompanied by schistose layers, which pre- 
 sent instructive examples of dynamic metamorphism. 
 
85 
 
 williams.] SCHISTOSE BANDS IN THE GREENSTONES. 
 
 The accompanying map (PL IV) represents an enlarged portion of 
 Major Brooks’s map of Lower Quinnesec Falls. Commencing at the 
 western corner of the basin there are, along its northern shore, three 
 bands of dark and two of light colored rocks. The two kinds of struct- 
 ure, massive and schistose, are so intimately connected in both of them 
 that it is impossible to escape the conviction that the latter has been 
 secondarily developed. 
 
 If we begin at the extreme western end of this exposure, at the corner 
 of the basin where a sharp bend in the river’s course has produced a 
 low, sandy beach, we discover that the rocks are of a dark green color. 
 The first specimen taken from this band (No. 11001) is massive and 
 jointed. No feldspar is visible, except in large porphyritic crystals, 
 which are not common. Even in this massive rock occasional narrow 
 bands, having a wavy foliation, may be seen. These resemble slicken- 
 sides, and represent planes of slipping or sliding in the massive rock 
 (No. 11002). Tracing these rocks a short distance to the east, the wavy 
 schistose bands become more and more numerous, until the whole mass 
 becomes decidedly slaty, and has a greasy feel. This foliated rock 
 strikes slightly south of east and dips steeply toward the north. The 
 laminae are frequently separated and bulged into lenses, which are 
 either filled with quartz or are still open and then coated with drusy 
 quartz (No. 11003). These slaty rocks have a dark gray color, and, in 
 some respects, resemble hydro-mica schists, but yet it is impossible to 
 separate them in the field from the dark green massive rocks above 
 described, as each passes by insensible gradations into the other. 
 
 Under the microscope, No. 11001 appears as a medium grained aggre- 
 gate of feldspar and pale, fibrous hornblende with some ilmenite and 
 leucoxene. The structure is still well preserved. The feldspar is in 
 stout, columnar crystals, all distinctly striated and often considerably 
 changed to zoisite or epidote. The hornblende is in irregular, ragged 
 masses or in minute needles. The pale, fibrous sort is plainly seen to 
 have been derived from a compact, darker green arid pleochroic variety ; 
 but farther back than this (i. e., to a possible original pyroxene) it can 
 not be traced. There is also a little pale green clilorite, looking much 
 like the secondary hornblende, except between crossed nicols, where it 
 is nearly isotropic. 
 
 No. 11002, taken from one of the narrow schistose bands, has plainly 
 been produced by a shearing or sliding within the last described mas- 
 sive rock, and presents an interesting relationship to it when placed 
 under the microscope. The two are plainly identical as far as the com- 
 ponent minerals are concerned, but the structure of the latter has under- 
 gone a great change. The grain at first glance appears to be finer, but 
 this is soon seen to be due to a crushing of the original minerals. The 
 feldspars especially are very much broken and their parts more or less 
 separated. This mechanical action has been attended by increased 
 chemical activity. The original substance of the crushed feldspar crys- 
 
86 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62 . 
 
 tals is hardly as much changed as in the preceding instance, but there 
 has been a considerable recrystallization of new feldspar substance 
 (probably albite). The hornblende, because of its secondary nature, is 
 more like that in the massive rock (No. 11001), but even this is some- 
 times sundered and torn. Chlorite is much more abundant, especially in 
 the interstices between the fragments of the broken feldspar crystals. 
 It is sometimes filled with very delicate and minute, though extremely 
 sharp, epidote crystals. The ilmenite is more extensively changed to 
 leucoxene than before, and, in some cases, shows a decided pulling out 
 in the direction of the schistose structure. On the whole, many of those 
 metasomatic changes which the greenstones most commonly show are 
 here seen to have been accelerated and intensified by the mechanical 
 force which has crushed the rock and so changed its structure. Thus 
 the two forces — dynamical and chemical — may go hand in hand and 
 together produce a rock which is both structurally and mineralogically 
 very different from that out of which it has been derived. 
 
 Passing eastward along this exposure, we next come to a wide band 
 of much lighter colored rock, which extends as far as the lower side of 
 the small cove, situated on the right bank immediately below the falls. 
 This band exhibits, in a most admirable manner, the secondary devel- 
 opment of schistose layers in a massive rock, and is well deserving of 
 careful study. The most typical and least altered form occurs just at 
 and below the corner of the small cove. This is a medium grained, 
 massive aggregate of opaque white saussurite and light green, fibrous 
 hornblende, and it closely resembles, in its external aspect, the barrier 
 rock at both Upper Quinnesec and Sturgeon Falls. Nos. 11008 and 
 11009 represent this occurrence, but even the most massive specimens 
 which could be obtained are seamed with cracks approximately parallel 
 in direction and coated with a lamellar, soft green mineral like that in 
 the adjoining schists. This is shown by examination to be chlorite. 
 On both sides of the massive portion of this band the parallel cracks 
 become more and more abundant (No. 11004 below, and No. 11010 
 above), and on the lower side of the small cove the rock passes, with- 
 out any break in its continuity, into silky schists (No. 11011), like those 
 above described from the opposite side of the river (cf. No. 11046, p. 84). 
 
 U nder the microscope, the least altered specimens of this rock (Nos. 
 11008 and 11009) are found to bear a close resemblance to the light 
 colored gabbro of Sturgeon Falls (see p. 68), except that in the present 
 instance no trace of diallage is discernible. The structure of the two 
 rocks is the same. The feldspar is here also replaced by the same gray, 
 opaque saussurite, in which, with a high power, zoisite and calcite may 
 be easily detected. The hornblende, as seen in a microscopic section; is 
 practically colorless. Only occasionally are traces of a greenish tinge 
 observable. Between crossed nicols this mineral generally exhibits a 
 homogeneous extinction, so that it can not be regarded as truly fibrous, 
 and yet there can be no doubt as to its secondary nature. Its edges are 
 
u. S. GEOLOGICAL SURVEY 
 
 BULLETIN NO. 62 PL. 
 
 Dark Diabase* 
 
 Light Schist^ 
 Dark Piabase^ T^I 
 Light Gabbro-diqrite 
 aftl se.ricite schists. 
 
 JarkDiabasi 
 aChlorite ; 
 Schists 
 
 WISCONSIN 
 
 T. 38JST.;R.20E. 
 
 M! I C H I G Ajn 
 T. 3 9 _N".;R -30 W. 
 
 MAP 
 
 of 
 
 LOWER QUINNESEC FALLS 
 
 Menominee River 
 (After Brooks) 
 
 SCALE 
 
 Fee i 
 
 ^Mile 
 
THt UW» W 
 Of ' Ht 
 
 mwersw of fu»o» 
 
WILLIAMS.] 
 
 EFFECT OF CRUSHING ON THE FELDSPAR. 
 
 87 
 
 ragged and there is a decided tendency to separation into fibers r even 
 when these are not actually present. It is noteworthy that this sec- 
 ondary hornblende can only be traced back (and that in rare instances) 
 into a more compact greenish or brownish variety of the same mineral. 
 In none of the thin sections is there any positive evidence that dial- 
 lage was ever present; and yet the close similarity of this rock to the 
 Sturgeon Falls gabbro naturally suggests it. If the diallage were 
 originally present it has completely changed to the pale hornblende, 
 while the brown hornblende longer resisted the bleaching action, and 
 hence sometimes still remains. If this were not the case, we are com- 
 pelled to assume one of the two other alternatives suggested in the 
 case of the porphyritic diorite from the other side of the river, No. 
 11098 (see p. 78). 
 
 The pale hornblende is often partially altered to colorless chlorite, 
 and the ilmenite is more or less changed to leucoxene. 
 
 Nos. 11004 and 11010, taken from either side of the above described 
 band, represent somewhat schistose varieties of it which have been 
 produced by the action of pressure , That this is actually the case 
 is admirably shown by a microscopic examination. The hornblende 
 of the original rock seems to have passed completely into a very pale 
 or colorless chlorite. Saussurite, on the Other hand, is less abundantly 
 developed than in the more massive rock above described, and it is dis- 
 posed in narrow veins or in small, irregular spots. The ilmenite has 
 given its place to a dark gray substance resembling leucoxene. This 
 is drawn out in stringers following the direction of the schistosity, 
 and in the center of these a yellow grain of rutile may sometimes be 
 observed. Galcite is also present. The structure of the rock is 
 completely different from that from which it is supposed to have been 
 derived. It is now composed largely of a fine grained groundmass. 
 This is made up of a microgranitic aggregate of minute grains of an 
 unstriated substance resembling quartz, but which, from its high spe- 
 cific gravity, is probably a feldspar. These grains, together with 
 chlorite scales, leucoxene, some calcite, and an occasional bit of epi- 
 dote or sericite, are arranged so as to produce an indistinct schistose 
 structure, the bands of which bend and wind around larger porphyritic 
 individuals of feldspar. In this way a lenticular or “ Flaser” structure 
 results, which, however, is hardly discernible, except under the micro- 
 scope. A very particular interest attaches to the porphyritic feldspar 
 crystals of these rocks. In comparison with those in the more massive 
 rock (11008 and 11009), they are but slightly altered to saussurite; in- 
 deed, for the most part, they are surprisingly fresh and glassy. Glis- 
 tening cleavage surfaces may be readily detected with the unaided eye, 
 and under the microscope this feldspar appears in clear, colorless grains, 
 almost wholly free from inclusions of any kind. Occasionally these 
 possess a light brownish tinge, due to some evenly distributed pig- 
 ment. Between crossed nicols this clear feldspar substance presents 
 sharp twinning lamella; and a comparatively high extinction angle. 
 
88 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62 . 
 
 The individual crystals are invariably broken and the fragments are 
 more or less separated. The intervening spaces are filled with a micro- 
 granitic ground in ass, as shown in Plate Till, figs. 1 and 2, of other 
 similar, though more acid rocks from Upper Quinnesec Falls and from 
 the vicinity of Marquette, Michigan. 
 
 The clearness and freshness of this feldspar would at first suggest the 
 probability of its being a secondary crystallization, as, for instance, 
 albite is often found to be. This, however, is shown not to be the fact, 
 first, by the broken state of all the crystals, indicating that they must 
 have been in existence when the rock was pressed and crushed ; and, 
 second, by their physical properties which show that the feldspar is 
 labradorite. Upon isolation this feldspar was found to have a specific 
 gravity of 2.69 ; and in cleavage pieces parallel the basal plane, it gives 
 an extinction augle of 12° to 20° on each side of the twinning- trace. 
 
 The survival of the original feldspar in an almost unaltered state, in 
 a rock so profoundly changed by mechanical action, naturally occa- 
 sioned some surprise. Examples of the same sort have already been 
 cited (e. g. Nos. 11154 and 11165 from Sturgeon Falls, and No. 11032 
 from the diorite ridge below Lower Quinnesec Falls), and so many cases 
 of a like character were encountered from other localities that the oc- 
 currence of the freshest feldspar in the most crushed rock must be re- 
 garded as the rule. 
 
 I know of no way of interpreting this phenomenon, substantiated by 
 so many instances, except by supposing that the pressure, which acts 
 powerfully in stimulating chemical action in the solid rock, is relieved 
 on the harder grains of a crushed band, since these are able to change 
 their position by slipping among the softer materials. 
 
 The nearly vertical, silvery schists (No. 11011) which occupy the west- 
 ern corner of the little cove just below the Lower Quinnesec Falls, rep- 
 resent only a more highly metamorphosed state of the rocks above de- 
 srcibed. They are extremely soft, fissile, and schistose in a hand-speci 
 men. Under the microscope they closely resemble the groundmass of 
 the last described rocks (Nos. 11004 and 11010). The granular aggre- 
 gate is so disposed as to produce a decided schistose structure. Both 
 calcite and sericite have become more abundant, while the porphyritic 
 feldspar crystals have completely disappeared. The leucoxene also can 
 nolougerbe found, but the long lines of very sharp and minute rutile 
 crystals, which are not present in any of the more massive related rocks, 
 appear to have taken its place. 
 
 The perfect continuity of the massive rock (Nos. 11008 and 11009) 
 with these schists, through the intermediate member (11010) is admira- 
 bly shown in the exposure at the western end of this small cove. 
 
 The following chemical analyses of these three specimens have been 
 made by Mr. K. B. Biggs. 
 
willtams] ANALYSES OF LOWER QUINNESEC GREENSTONE. 89 
 
 I. No. 11008, Gabbro-diorite from Lower Quinnesoc basin. 
 
 II. No. 11010, Schistose form of the same rock. 
 
 III. No. 11011, Seriate schist adjacent to last. 
 
 
 (I.) 
 
 (II.) 
 
 (III. ) 
 
 Si0 2 
 
 47. 96 
 
 49. 19 
 
 46.21 
 
 ai 2 o 3 
 
 16. 85 
 
 18. 71 
 
 18. 38 
 
 FfrjOj 
 
 4. 33 
 
 5. 03 
 
 3. 30 
 
 FeO 
 
 4. 17 
 
 4.04 
 
 3. 90 
 
 CaO 
 
 13. 25 
 
 5. 92 
 
 6. 28 
 
 MgO 
 
 9. 15 
 
 7. 98 
 
 7. 03 
 
 Xa 2 0 
 
 1. 25 
 
 1. 44 
 
 2. 14 
 
 K 2 0 
 
 -.30 
 
 .77 
 
 .35 
 
 H 2 0 
 
 2. 89 
 
 5. Q£ 
 
 3. 82 
 
 C0 2 
 
 .08 
 
 1.82 
 
 8. 32 
 
 Total 
 
 100. 23 
 
 99. 95 
 
 99. 73 
 
 Ti0 2 not determined. 
 
 The close agreement between these analyses is striking. The low 
 percentage of iron sufficiently accounts for their uniformly light color. 
 The most striking difference is perhaps the loss of calcium and the 
 lesser loss of magnesium, both of which were undoubtedly carried off 
 in the form of soluble carbonates when the rock was crushed. The 
 water is contained in the pale chlorite, which first increases in amount 
 and then decreases, as its components are transformed into carbonates. 
 The sodium was first contained in the feldspar and the steady increase 
 in its relative amount is probably due to the development of the sericite- 
 like mica, which may be a paragonite. 
 
 It is interesting to compare the first of these analyses with that of 
 the Sturgeon Falls gabbro (I on p. 76), the close resemblance of which 
 to the rocks here under consideration has already been alluded to. 
 The only noticeable difference is a slightly larger proportion of silica 
 and a smaller proportion of alumina and lime in the Sturgeon Falls 
 rock. 
 
 Passing now still farther to the eastward, we come to the second band 
 of dark-colored greenstones (see map, PI. IY). These follow directly 
 after the narrow exposure of the above-mentioned silvery schists in the 
 western corner of the little cove and form a great part of its northern 
 shore. They resemble the rocks occurring in the band first described, 
 and present both massive and schistose varieties, which grade insensibly 
 into each other in a manner not less instructive than that in the two 
 bands already considered. 
 
 Nos. 11012, 11013, and 11021 (the first two from massive portions of 
 this band along the shore of the small cove; and the last from the Wis- 
 cousin side of the river directly opposite the falls) are essentially identical 
 in appearance and composition. In the hand-specimen they form a 
 compact, aphanitic mass, of a dark green color. Under the microscope 
 the originally diabasic nature of the rock is at once apparent, although 
 
90 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62. 
 
 the extensive mineralogical changes which have gone on have greatly 
 obscured its former structure. The components now present are al- 
 most wholly secondary. These are hornblende, chlorite containing epi- 
 dote, quartz, and leucoxene. Ilmenite and occasional traces of feldspar 
 are the only original constituents which remain. Still the disposition of 
 the secondary minerals is such as to outline a diabasic or ophitic struct- 
 ure often with great distinctness. The feldspar is rarely well pre- 
 served $ but a narrow zone of the unaltered substance of this mineral 
 often outlines a stoutly lath-shaped crystal, even when its interior is 
 wholly changed to an aggregate of quartz, chlorite, and epidote. The 
 hornblende has a curious appearance. Its crystals are brownish and 
 nonpleochroic with a somewhat granulated surface, so that it exter- 
 nally resembles diallage. Its cleavage and optical properties prove it 
 to be undoubtedly hornblende, although this superficial likeness to di- 
 allage is so strong as to almost compel the conviction that it has origi- 
 nated by paramorphism from a pyroxene. This brown hornblende is 
 seen with a high power to be gradually changing to a green variety, in 
 which a pleochroism for the first time becomes apparent. This also 
 frequently passes over into a fibrous hornblende. The chlorite epidote 
 aggregate in these rocks is very finely developed. The chlorite is of 
 an emerald green color and distinctly pleochroic. It appears between 
 crossed nicols as isotropic or polarizes with a maroon tint. The epidote 
 is in sharp, light yellow crystals, with the characteristic shape and op- 
 tical properties of this species. The microscopic appearance of this 
 aggregate is represented in PI. XI, fig. 1, drawn from a specimen 
 collected below the Upper Quinuesec Falls (No. 11049). The literature 
 relating to it has already been cited (Chapter I, p. 57). The epidote 
 crystals have been described from the Menominee region by Wichmann 1 
 and others as secondary augite. This chlorite epidote aggregate covers 
 considerable areas and occupies the place of both the feldspathic and 
 the pyroxenic constituents. In addition to the minerals already named, 
 ilmenite, with its leucoxene border, pyrite and secondary quartz are 
 quite abundant in these rocks. 
 
 No. 11014, taken from a narrow, schistose band in the massive green- 
 stone (No. 11013), shows in a remarkably clear manner how the dy- 
 namic metamorphism of this rock has been accomplished. In this in- 
 stance there can not be the least doubt as to the continuity of the rock- 
 mass. The hand-specimen No. 11014 has a decidedly schistose struct- 
 ure, and under the microscope it shows the effects of mechanical crush- 
 ing and attendant mineralogical changes, with great distinctness. The 
 whole rock, with the exception of certain remains of the larger feldspar 
 crystals, has been reduced to. a fine grained mass, showing an aggre- 
 gate polarization. Light green chlorite has been largely developed and 
 has completely replaced all the bisilicate elements. The parallel ar- 
 rangement of the scales of this mineral is what produces the schistose 
 
 1 Geol. Wisconsin, vol. 3, 1876, pp. 623, 624. 
 
Williams] ANALYSES OF LOWER QUINNESEC GREENSTONE. 91 
 
 structure, and it surrounds and incloses the small grains in the man- 
 ner which has already been explained in connection with No. 11031 
 (p. 81 ) and illustrated in PI. IX, fig. 2. The clear, secondary grains form- 
 ing this mosaic are certainly, to some extent at least, quartz, while a 
 portion of them may be an unstriated feldspar. Cal cite has been 
 largely developed in the schistose rock, and the leucoxene is replaced 
 by rutile, either in stout, yellow grains, or in minute, sharp crystals ar- 
 ranged in long, sinuous lines. 
 
 The mechanical action which produced this schistose band has there- 
 fore resulted in the crushing of the rock, and the almost total disap- 
 pearance of all of the original components. The comparatively slight 
 change in the chemical composition of the rock as a whole may be seen 
 from the two following analyses of Nos. 11021 and 11014, made by Mr. 
 B. B. Biggs. 
 
 I. No. 11021. Dark massive greenstone, Lower Quinnesec Falls. 
 
 II. No. 11014. Dark schistose greenstone, forming a band in the last. 
 
 
 (I.) 
 
 (II.) 
 
 Si0 2 
 
 43. 80 
 
 44. 49 
 
 A1 2 O s 
 
 16. 08 
 
 16. 37 
 
 Fe 2 0 3 
 
 9. 47 
 
 5. 07 
 
 FeO 
 
 10.50 
 
 5. 50 
 
 CaO 
 
 7. 81 
 
 7.94 
 
 MgO 
 
 6. 54 
 
 7.50 
 
 Xa. 2 0 
 
 1.96 
 
 2. 59 
 
 K 2 0 
 
 0. 34 
 
 0. 56 
 
 H 2 0 
 
 3. 99 
 
 4.99 
 
 C0 2 
 
 0. 08 
 
 5. 38 
 
 Total 
 
 100.57 
 
 100. 39 
 
 Ti0 2 not determined. 
 
 Powder dried at 105° C. 
 
 The changes here are at once seen to be due (1) to the total removal 
 of the iron ores (loss of iron) ; (2) to the production of carbonates 
 (gain of C(> 2 , carbonatization) ; and (3) to the increase in the amount of 
 chlorite, (increase of H 2 G, hydration). 
 
 Toward the eastern end of the small cove the dark-green schistose 
 rocks appear to pass by insensible gradations into exactly similar ones 
 of a lighter color. No. 11015, one of these, is seen under the micro- 
 scope to be a very schistose aggregate of extremely pale chlorite and 
 quartz grains. There is a little calcite here present and occasional 
 scales of sericite. The rutile, in very minute and sharp crystals, is here 
 crowded into long bands and stringers which follow the schistosity of 
 the rock and give the thin section a pronounced “Flaser” structure. 
 
 No. 1 101 G, from the extreme eastern corner of this cove, represents a 
 band of lightcolored brownish rocks with a perfectly developed schis- 
 tose structure and a grain somewhat resembling that of wood. These 
 
92 
 
 GREENSTONE SCHIST AREAS OP MICHIGAN. 
 
 [bull. 62 . 
 
 stand nearly vertical, though some dip from 65° to 70° N. 20° W. 
 Their strike is turned from that of the other rocks here (S. 70° E) some 
 30° to 40°, so that they now strike N. 70° E. Under the microscope 
 this rock is seen to have essentially the same structure and composition 
 as the last. The main difference between them is that the present spec- 
 imen has a brown chlorite instead of a green one. This it is that im- 
 parts the peculiar color to the rock in the hand-specimen. There is 
 also more calcite in this rock than in the other. It would seem, along 
 with No. 11011 above described, to represent the most profoundly met- 
 amorphosed phases of the massive rocks at Lower Quinnesec Falls. 
 
 The original constituents have undergone an alteration to chlorite, 
 quartz, carbonates, and rutile. The iron has largely disappeared, and 
 the crystallization of the new components under lateral pressure has 
 produced a very pronounced schistose structure. 
 
 No. 11023, from the upper end of the breakwater, above the falls 
 (Wisconsin side), is very closely allied to the two specimens last de- 
 scribed. It is a grayish schist, with the prevailing strike, but every- 
 where seamed with transverse cross-gashes, which are, for the most part, 
 filled with infiltrated quartz. There seems to be little doubt from a 
 field examination, that this rock is continuous with the massive diabase 
 (No. 11021) in the same way that the last mentioned specimens are con- 
 tinuous with Nos. 11012 and 1 1013. The massive green rock (No. 11021) 
 is exposed a very short distance to the west of it, where it also is filled 
 with seams and cross-gashes, which appear to have been squeezed open 
 by lateral pressure. From this point the transition to the gray schis- 
 tose rock is a very gradual one. The latter rock has no regular bedding 
 but only a cleavage in one direction. This causes it to break out in angu- 
 lar prisms. The rock is everywhere fissured, slickensided, and filled 
 with infiltration quartz, as evidence of the enormous pressure to which 
 it has been subjected. Under the microscope it is much like No. 11016. 
 There is the same quartz mosaic, pale chlorite and strings of rutile 
 needles, arranged so as to produce a decided schistose structure. There 
 is, however, in this rock considerably more calcite and an additional 
 feature in the way of remains of former feldspar crystals. These are 
 considerably altered, and appear to be changing to a mass quite like that .* 
 which composes the rest of the rock. In fact, this has gone so far that 
 it is almost impossible to distinguish these feldspars in ordinary light, 
 although their outline and nature become very apparent between crossed j 
 nicols. They are arranged without reference to the present schistose 
 structure of the rock, and evidently represent original constituents of 
 the rock from which the present schist has been derived. 
 
 In place of the above-described transition from massive to schistose 
 rocks along a line — normal to the strike — there is in many instances the 
 st-ill more conclusive proof to be found in this same transition around 
 ellipsoidal or lenticular cores of massive rocks. Such masses grow grad- 
 ually schistose around their periphery and pass into schists which ap- 
 
Williams.] SCHISTOSE LAYERS SURROUNDING MASSIVE CORES. 
 
 93 
 
 pear to wind around and enclose them, but which, in reality, have been 
 formed out of their own substauce. An admirable example may be 
 seen just at the Wisconsin edge of the river at the foot of Lower Quin- 
 nesec Falls. This is a lenticular mass of massive greenstone about eight 
 feet in its longest diameter. This grades insensibly around its edge, 
 into dark green schists, differing only in their structure from the cen- 
 tral rock. Four specimens (Nos. 11017, 11018, 11019, and 11020) were 
 collected to illustrate this passage. The most interior and massive one 
 (No. 11017), although to all appearances quite compact, is found upon a 
 microscopic examination to be wholly altered mineralogically. The 
 bisilicate constituents are now represented only by a light emerald- 
 green, pleochroic mineral, which, in spite ot its comparatively strong 
 action upon polarized light, is probably chlorite. This frequently con- 
 tains sharp epidote crystals. The feldspar, while retaining much of its 
 original form, is composed either of a gray, opaque saussurite or of a 
 fine mosaic of quartz and albite grains and a great deal of calcite. 
 
 The extremely altered condition of the central portion of this core is 
 perhaps rather advantageous than otherwise, for, while there can be no 
 doubt as to its original character, the transition to the schists is seen to 
 take place wholly by a change in structure, without further mineral- 
 ogical alteration. 
 
 No. 11018, taken from a place where indications of a schistose structure 
 are already quite apparent, shows just the same mineral components as 
 the last. The chlorite scales, however, have assumed a decidedly par- 
 allel arrangement, which is followed, to a less extent, by the fine mosaic 
 of quartz and albite grains. The calcite is better crystallized, and forms 
 larger individuals. There are also present some minute scales of a deep 
 red iron oxide, probably gothite, or limonite. The gray saussurite is 
 likewise common. 
 
 No. 11019, in which the schistose structure is still more apparent, 
 shows the same components as the others. The parallel arrangement 
 of the chlorite is still more pronounced and the calcite still better crys- 
 tallized. Strangely enough, we meet here, in a very schistose rock, 
 better preserved feldspar crystals than can be found in the more massive 
 greenstone, with which it is so intimately connected. This is but one 
 more instance of the remarkable rule set down on p. 88, and alluded 
 to several times already. This thin section (No. 11019) exhibits feldspars 
 so well preserved that only occasional epidote crystals are developed 
 in them. There is also to be seen a remarkably good example of the 
 change of pyrite to iron hydroxide. 
 
 No. 11020 represents the extreme member of this series. It is a typical 
 chlorite schist, in which alternating and interlacing areas of pale green 
 chlorite and a fine quartz albite mosaic may be seen. In both a highly 
 developed schistosity is produced by the parallel arrangement of the 
 components. The grain of this rock, in so far as it is due to these alter- 
 nating areas, appears somewhat coarser than in the less altered forms* 
 
94 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [PULL. 63 . 
 
 The chlorite, if it be examined with a higher magnifying power, is seen 
 to be filled with irregular spots of a reddish brown color, which feebly 
 polarize, and seem to be the remains of former feldspar crystals. Rutile 
 in grains or sharp crystal forms is also present. 
 
 The fine mosaic which composes the other areas, contains, in addi- 
 tion to the quartz and albite grains, calcite and chlorite in small, elon- 
 gated scales. 
 
 A careful field examination shows conclusively that the four speci- 
 mens here described (Nos. 11017 to 11020), represent only different 
 forms of the same rock. In fact, the mineral composition is identical 
 for all, although the most massive form is beyond all doubt an altered 
 diabase, while the exterior bands, which surround this core are just as 
 truly examples of a typical chlorite schist. 
 
 No. 11048 is a specimen of the massive, dark green rock which has 
 been blasted out behind the shanty on the Michigan side of Lower 
 Quinnesec Falls. A microscopic examination shows at once that this 
 rock was originally a diabase, although its present constituents are 
 for the most part secondary. The shapes of the original minerals are 
 indistinctly outlined, and so the structure of the rock is preserved. 
 There is now present a pale green hornblende, probably secondary to 
 pyroxene, although no traces of this mineral are preserved ; epidote, 
 chlorite, saussurite and leucoxene in zones around the titanic iron. 
 The feldspar has rarely changed to the opaque, gray saussurite, but is 
 replaced for the most part by a mass of sharply defined epidote crys- 
 tals. Where the feldspar and hornblende have jointly contributed to 
 the formation of secondary products, we have the chlorite epidote 
 aggregate as a result. A little secondary quartz is also observable. 
 
 The two remaining specimens examined from Lower Quinnesec Falls 
 (Nos. 11101 and 11102) were collected on the Michigan side of the river 
 above the fall, from two xmints designated by u and w respectively on 
 Major Brooks’s map. They exhibit in a marked degree the effects of 
 stretching upon massive greenstones. If a rock mass were subjected 
 to a great lateral pressure when it was free to expand in a direction 
 perpendicular to that in which the pressure acted, it would appear as 
 though it had been subjected to a strain or tension in the direction along 
 which it was free to move. There would be a breaking and pulling out 
 of the individual minerals into parallel bands along the line of expan- 
 sion or apparent stretching. This phenomenon is very admirably dis- 
 played in these two specimens. 
 
 No. 11102 is the coarser grained of the two rocks and shows its struct- 
 ure best when the microscopic section is examined with a pocket-lens. 
 Its appearance, as seen under a low power of the microscope, is por- 
 trayed in PL XI, fig. 2. One of the most important of the original 
 constituents of this rock was a triclinic feldspar in large sized indi- 
 viduals. These are now fissured in a direction normal to the stretch- 
 ing and their fragments are separated in a most striking manner. The 
 
williams.] STRETCHING OF ILMENITE IN GREENSTONE. 95 
 
 interstices are filled with long, chlorite scales arranged perpendicular 
 to the walls of the fissures,* more rarely calcite replaces this chlorite. 
 Here again we have clear evidence that the chemical change in the 
 feldspars of rocks which have been subjected to great mechanical action, 
 is comparatively slight. The feldspars of this rock are scarcely altered 
 except by being broken or crushed. 
 
 The grains of original quartz in this rock have suffered the usual de- 
 formation, being rarely brokeu but more frequently in a state of ten- 
 sion which imparts to them an undulatorv extinction. 
 
 Very finely fibrous, dark green aetinolite is quite abundant, repre- 
 senting some other bisilicate constituent (either pyroxene or compact 
 hornblende) all traces of which have now disappeared. The fibers are 
 sometimes parallel over considerable areas, sometimes crowded together 
 into a confused and matted mass. They themselves show no evidence 
 of pressure and hence must have originated during the action of the 
 pressure or subsequent to it. The former is the more probable and the 
 pressure may have been the very cause to which the hornblende owes 
 its origin, as I suggested in a former paper. 1 
 
 None of the constituents displays the effects of the stretching action 
 to which this rock has been subjected more distinctly than the ilmen- 
 ite. This mineral is abundant in grains of considerable size, all of 
 which have been irregularly fissured in a direction transverse to the 
 tension and the fragments separated, exactly like those of the feldspar. 2 
 (See PI. XI, fig. 2.) The absence of leucoxene around these grains may 
 indicate that in this case also the chemical action is inversely propor- 
 tional to the mechanical. 
 
 No. 1X101 is a very similar rock of a finer grain, in which the effects 
 of stretching are not so apparent. We therefore find the chemical al- 
 teration of the feldspar proportionately greater. This mineral is not 
 so much broken as in the specimen last described, but it is filled with 
 secondary crystallizations of chlorite and epidote. The ilrneuite is 
 broken and stretched in the manner described in the preceding speci- 
 men, though to a less degree. The separated ilmenite fragments, how- 
 ever, in this case present a contrast to the others, in having leucoxene 
 quite abundantly developed around them. The hornblende of this 
 rock is both brown and green ; each variety is dark colored and in- 
 tensely pleochroic. Most of it is fibrous, the fibers following in their 
 arrangement the general direction of the foliation. 
 
 1 Am. Jour. Sci., 3d Berios, Oct., 1884, vol. 28, p. 266. 
 
 2 A. Schenck describes and figures exactly this phenomenon in the schistose diabases of the upper 
 Kuhr Valley. Inaugural Dissertation, Bonn, 1884, p. 55. 
 
CHAPTER III. 
 
 GREENSTONE BELTS OF THE MENOMINEE DISTRICT— (Continued). 
 
 UPPER OR BIG QUINNESEC FALLS. 
 
 About 3J miles above Lower Quinnesec Falls, described in the 
 preceding chapter, the course of the Menominee River is again 
 interrupted by extensive rock exposures, which skirt the banks for 
 nearly 2 miles. The upper mile of this distance is a high, rocky gorge, 
 known as the u Horse Race,” through which the water rushes and 
 tumbles in a foaming rapid. The current then flows more quietly 
 through a broader, though still rocky channel, for half a mile, when 
 it suddenly plunges over a fall of considerable height and beauty, known 
 as Upper or Big Quinnesec. 1 
 
 Below this fall the stream broadens into a wide basin, which is also 
 bordered by rocky shores. 
 
 The continuous exposure of Upper Quinnesec Falls is, therefore, 
 separable into three naturally distinct divisions. These divisions are, 
 moreover, each characterized by a different kind of rock ; a fact which 
 serves to distinguish them almost as sharply as their physical confor- 
 mation. (See map, PI. Y.) 
 
 The rocks which are exposed along the basin belong, for the most 
 part, to the class of dark, more or less schistose greenstones, similar to 
 those occurring at Lower Quinnesec Falls. These were once diabases 
 rich in iron, which have produced amphibolitic and chloritic schists of 
 a deep green color. 
 
 The actual barrier at Upper Quinnesec Falls is, on the other hand, com- 
 posed of the light colored type of greenstone with a distinctly granular 
 structure, like that already described as occurring at both the Sturgeon 
 and Lower Quinnesec Falls. This is also the commonest rock for the 
 half mile above the falls, before the rapid is reached. It is deserving 
 of careful study on account of the transition which it presents into 
 light colored sericite schists. 
 
 The rock which forms the steep walls of the gorge known as the Horse 
 Race is of still a different type. It will receive a separate treatment, 
 as it is quite unlike anything observed elsewhere in the Menominee 
 Valley. 
 
 1 This name is a corruption of the Chippewa Bequenesec which is spoiled by H. Credner in his descrip- 
 tion of this locality as Bekuenesek. (Neues Jahrbuch fur Mineral., 1870, p. 971.) 
 
 96 
 
u. s. geological survey 
 
 BULLETIN NO. 82 PL. V 
 
 Schistose 1 
 
fHt UWM« 
 
 Of fHt 
 
williams.] GREENSTONES BELOW UPPER QUINNESEC 1 FALLS 
 
 97 
 
 Finally bands of certain acid rocks— granites, gneisses, and schistose 
 porphyries — occur in the greenstones both at the fall and along the 
 Horse Race. They appear to stand in the closest genetic relation both 
 to each other and to the great granite area which lies south of the river 
 and approaches it at this point more nearly than at any other. 
 
 We may, therefore, consider the rocks of Upper or Big Quinnesec 
 Falls under the four following heads: 
 
 (1) The dark colored greenstones of the basin. 
 
 (2) The light colored greenstones at the falls. 
 
 (3) The coarse grained diorites of the Horse Race. 
 
 (4) The acid rocks, both massive and schistose. 
 
 THE DARK COLORED GREENSTONES OF THE BASIN. 
 
 At the lower (eastern) extremity of the basin, below Upper Quinnesec 
 Falls, is an exposure of greenstone which juts into the river from the 
 Wisconsin side. It is of a uniformly green color and, for the most part, 
 massive, although schistose portions are not infrequent, which have the 
 X>revailing strike, N. 70° W., and stand nearly vertical. These schist- 
 ose bands have in the field every appearance of being secondary 
 since they are only locally developed and grade imperceptibly into 
 the massive rock. A specimen from this locality, No. 11049, when ex- 
 amined microscopically, appears to be very similar to a rock already 
 described from the Lower Falls (No. 11048). The process of alteration 
 there indicated, however, has here progressed much further. There is 
 every reason to believe that this rock, like the other, was once a diabase; 
 and yet, in this case, all traces both of the original structure and of the 
 original constituents have disappeared. The feldspar substance is com- 
 pletely replaced by a confused network of epidote needles, or of these 
 mixed with chlorite; some rather compact, green hornblende still re- 
 mains, but this mineral is rapidly disappearing, and the manner in 
 which, jointly with the feldspar, it furnishes the materials out of which 
 the chlorite-epidote aggregate is formed is here very instructively dis- 
 played. In fact, no other rock showed this characteristic form of altera- 
 tion as well as this one, and it was therefore selected to furnish the 
 illustration. (See PI. XI, fig. 1.) The titanic iron is here in the form of 
 small grains, accompanied by leucoxene. 1 
 
 On the southern or Wisconsin side of this basin there are no more 
 important exposures of the dark colored greenstones. On the Mich- 
 igan side, however, such exposures are abundant and have been in- 
 dicated on Maj. Brooks’s map as the points 0 , au, bb , and cc. 2 
 
 Two suites of specimens collected at these points, one by Prof. Irving 
 
 1 Slide No. 931 of the collection of the Lake Superior Division of the U. S. Geological Survey was 
 prepared from a specimen collected by Prof. It. D. Irving west of the above, among the light colorod 
 greenstones. It is of great interest in this connection because its feldspar is quite well preserved and 
 shows in a most unmistakable manner the ophitic structure of tho diabases. In other respects espec- 
 ially in the character and abundance of the epidote-chlorite aggregate, it is quite identical with No. 
 11049. 
 
 a Geol. Wisconsin, vol. 3, PI. 3, p. 474, • 
 
 Bull 62 7 
 
98 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 •[BULL. 62 . 
 
 and the other by the writer, were studied. The rocks all exhibit the 
 effects of extreme mechanical action upon their constituents, which has 
 so far obliterated their original structure as to render their true char- 
 acter doubtful. They agree in being composed of different proportions 
 of a much crushed and altered, reddish brown feldspar and a pale green 
 mass consisting of chlorite aud quartz. The latter aggregate is of sec- 
 ondary origin and imparts a cleavage to the rock, since the chlorite 
 flakes are all arranged in one direction. 
 
 No. 4162, from Prof. Irving’s collection, was the only specimen studied 
 microscopically from poiut z. It is composed mostly of feldspar, and 
 has, therefore, a reddish color. This constituent is intensely crushed 
 and its substance is so highly altered as to appear to grade imperceptibly 
 into the quartz chlorite matrix, which is present in small amount be- 
 tween its fragments. Scattered through this mass in the direction of 
 its foliation are long lines of some opaque iron oxide, accompanied by 
 very minute though sharply defined crystals and twins of rutile (Thon- 
 schiefernadeln), like those represented in Fig. 12, p. 106. In some cases 
 the iron oxide is absent, and these dark bauds may be seen with a high 
 magnifying power to be made up entirely of the closely clustered rutile 
 crystals. 
 
 Nos. 4163 aud 11070 are both from Brooks’s poiut aa, which he de- 
 scribes (loc. cit.) as composed of a u chloritic greenstone schist, with 
 pinkish grains of feldspar (Schalstein?).” 
 
 The first of these sections belongs to Professor Irving’s collection, 
 and exhibits under the microscope the effects of the crushing aud 
 stretching in a very marked degree. Its structure resembles that of 
 specimen No. 11102 from the lower Quinnesec Fall, described on p. 94", 
 and represented in PI. XI, fig 1. White and reddish feldspar crystals, 
 quartz grains, and opaque black spots of iron oxide are imbedded in a 
 secondary matrix consisting of chlorite, quartz, and epidote. No trace 
 of an original bisilicate now remains. All of the older components, 
 especially the feldspar and iron oxide, are much broken and their frag- 
 ments are separated in one uniform direction corresponding to the folia- 
 tion of the rock ; but yet the fragments which once belonged together 
 can still be recognized. The feldspar substance, in spite of the in- 
 tense crushing, is still remarkably fresh and its twinning striatiou dis- 
 tinct. Lath-shaped forms, like those of diabase, are present, though all 
 traces of the original rock structure have disappeared. The opaque 
 grains of iron oxide (magnetite) are broken aud pulled apart like the 
 feldspar and can be seen with a high magnifying power to be fringed 
 with minute and imperfectly formed rutile crystals. Sharply defined 
 octabedra of magnetite — evidently of secondary origin, as they never 
 exhibit any traces of mechanical action — are also scattered through 
 the chlorite, and in some cases these octahedra are crowded together 
 with little rutile crystals, both looking as though they had resulted from 
 the alteration of some ineexistiug mineral. 
 
WILLIAMS.] 
 
 RUTILE IN ALTERED DIABASE. 
 
 !)!) 
 
 No. 11070, collected by the writer from the .same locality as the last 
 (Brooks’s point aa ), possesses a similar character, though with -certain 
 important differences. The hand-specimen is dark green in color and 
 decidedly schistose. Under the microscope it is seen to he essentially 
 the same rock as that last described, but in an even more advanced 
 stage of alteration. The fragments of reddish feldspar, which can still 
 be seen to belong together, are here, as before, separated in the direction 
 of the foliation, while the spaces between them are filled with chlorite 
 flakes and quartz grains. The feature of particular interest in this speci- 
 men is, however, the abundance of its rutile and the constant and close 
 association of this mineral with the black iron oxide. This association, 
 as well as the general appearance of this rock under the microscope, 
 is represented in PI. XIII, fig. 2. The opaque, black grains, which in 
 reflected light can be seen to be intergrown with a considerable propor- 
 tion of pyrite, are surrounded by a border of stout, brownish yellow 
 needles, averaging from 0.1 to 0.05 mm in length by from 0.02 to 0.01 mm 
 in width. They are crowded closely together and are often parallel to 
 the external edges of the grains. Xot infrequently, also, they exhibit 
 a regularity of arrangement, crossing each other at angles approaching 
 60° and 120°. It will be readily seen, however, that in a random sec- 
 tion of the rock it is impossible to decide whether these are exactly the 
 angles or whether they are the angles 54° 43' and 65° 35' (with their 
 supplements, 125° 17' and 114° 25'), which von Lasaulx has shown are 
 produced by the twinning of rutile, and characteristic of its network 
 growth called as sagenite. 1 An isolation of these needles was made by 
 dissolving all the other constituents of the rock in HOI and HF, for 
 the purpose of obtaining material which might positively decide this 
 point, but no definite results were obtained. The needles are for the most 
 part irregular in their arrangement, and it still remains uncertain whether 
 their occasional regularity is due to twinning or to some other cause. 
 
 A chemical examination of the isolated needles showed that they were 
 composed of titanium oxide, while their crystallographic and optical 
 properties observed under the microscope proved them to belong to the 
 species rutile. 
 
 The fact that the black, opaque constituent of this rock is traversed 
 by parallel cracks and fissures, often in sets intersecting at an angle df 
 60°, like those observed in titanic iron, taken in connection with the 
 close relationship of the rock itself to the family of diabases, naturally 
 led to the assumption that the iron oxide was ilraenite. Moreover, the 
 similarity of the distribution of the rutile about the black cores to that 
 of leucoxene about ilmenite crystals in the process of alteration — its 
 presence its a continuous border and in every crack, while the black 
 substance itself is quite free from the needles 2 — seemed further to iudi- 
 
 1 Zoitschr. fur Kryst. u. Miu., vol. 8, 1384, p. 56. 
 
 2 This was shown, not merely by the absence of the larger needlos which, if they wore present, 
 must have appeared through the black substance of the iron oxido in the thin section, but also by 
 slowly dissolving away the oxide with HC1 under tho microscope and the failure thus to discloso any 
 Smaller crystals ot rutile, which might have been wholly inclosed within the black ore. 
 
100 GREENSTONE SCHIST AREAS OF MICHIGAN. | bull. 62. 
 
 cate the secondary origin of the rutile out of the ilmenite. This is the 
 view that was at first taken by the writer and published by him in a 
 letter to the Neues Jahrbuch fur Mineralogie, etc., 1887, vol. 2, p. 
 203. In a subsequent paper on the same rock, 1 Prof. Oathrein of Karls- 
 ruhe showed, among other points which he considered as objec- 
 tions to the secondary origin of the rutile, that the black iron oxide 
 was not ilmenite at all, but magnetite. This determination has since 
 been confirmed by a careful chemical examination made at my request 
 by Prof. S. L. Penfield, of the Sheffield Scientific School at New Haven. 
 
 A very similar occurrence of rutile needles, though inferior in size to 
 those here described, has been observed by Oathrein in the leucoxeue 1 
 border which surrounds both ilmenite 2 and titaniferous magnetite 3 in 
 certain Tyrolese rocks. Dr. J. Blaas also encountered the same kind 
 of a network of rutile crystals in a quartz phyllite from the neighbor- 
 hood of Innsbruck, but in this case it was unaccompanied by any opaque 
 ore. 4 In none of the instances observed by him does Oathrein consider - 
 the rutile as even possibly a secondary product. On the other hand, 
 he thinks that the little needles were formed simultaneously with the 
 ilmenite or magnetite, and that they have always existed in their pres- 
 ent form within the iron oxide, until more or less completely liberated 
 by the solution and removal of the latter. 
 
 In his article on the Quinnesee rock above cited, none of the points 
 insisted upon by Oathrein appear to militate against the secondary origin 
 of the rutile, except the last. As has been stated above, it is impossi- 
 ble in a random section to determine with certainty whether the nee- : 
 dies intersect at angles of exactly G0° and 120°, or at those so nearly 
 like them produced by twinning. But whichever be true, it is certain 5 
 that a large majority of the needles are quite irregular in their arrange- 
 ment. The discovery, however, that the black iron oxide which ac- 
 companies the rutile is not ilmenite but a magnetite almost free from ' 
 titanium, seems at first altogether incompatible with the idea that the 
 rutile is a secondary derivative from ilmenite. Nevertheless, a continued 
 and repeated study of a large number of thin sections of this rock have , 
 served to convince the writer more and more that the rutile was at 
 least not a constituent of the rock in its original state. The rutile ag- 
 gregates are never drawn out in the direction of the stretching, as are 
 all of the original constituents, notably the feldspar, and as they must 
 have been had they always been present in the rock. It is necessary, " 
 therefore, to assume that they originated subsequent to, or, more prob- 
 ably, at the time of the metamorphism. 
 
 The constant and intimate connection between the rutile and the 
 magnetite clearly shows that they are in some way genetically related. 
 Opposed to the supposition that they were originally parallel inter- 
 
 1 Neues Jahrbuch fur Mineral., etc., 1888, vol. 2, pp. 151-165. 
 
 2 Zeitschr. fur Kryst. u. Miu., vol. 6, 1882, p. 248. 
 
 3 Ibid., vol. 8, 1884, p. 321. 
 
 4 Tschormak’s min. u. petrog. Mittheil,, vol. 4, 1882, p. 514, fig. 2. 
 
 . 
 
 — 
 
WILLIAMS.] 
 
 PROBABLE ORIGIN OP THE RUTILE. 
 
 101 
 
 growths, is, however, the fact that the rutile needles never occur within 
 the magnetite, now present. The rutile forms a border around the black 
 areas, which themselves frequently show a sharp crystal outline, diffi- 
 cult to reconcile with the idea that they have been partially dissolved 
 so as to reveal the rutile which once existed within them. In one in- 
 stance, indeed, an aggregate consisting of rutile needles and sharp oc- 
 tahedra of magnetite was observed, but this is exceptional. On the 
 other hand, it may often be clearly seen that the magnetite has, to a 
 greater or less degree, been removed by solution ; but in all such cases 
 the place that it once occupied exists within the fringe of rutile, but is 
 itself wholly free from the needles. This space is often filled with cal- 
 cite, or some similar carbonate, in slightly radiating tufts. 
 
 All of these observations seem to point to a contemporary origin for 
 both the magnetite and rutile from some preexisting mineral, which in 
 the present case may very probably have been ilmenite. 
 
 The change of hematite into magnetite is one which has been often 
 observed. Roth 1 quotes descriptions of this alteration from Breithaupt, 
 Volger, Peters, vom Rath, Petersen, Doll, Grattarola, and Zeparovich. 
 There seems to be no reason why the corresponding titaniferous com- 
 pound, ilmenite, should not also pass over into magnetite with the 
 separation of its titanium in the form which is most stable for the con- 
 ditions then prevailing. 
 
 Rutile is well known to be widely distributed in microscopic crystals 
 through schists which have resulted from the regional metamorphism 
 of both sedimentary and eruptive rocks. It must therefore be a com- 
 pound well in accord with the conditions producing metamorphism. 
 
 The common presence of rutile needles in diabase rocks which have 
 been intensely altered by pressure, and its absence in their unaltered 
 forms, in connection with the fact that the original ilmenite disappears 
 in proportion as the rutile is developed, has inclined such eminent 
 petrographers as Lossen and Rosenbusch to the supposition that the 
 latter mineral has originated from an alteration of the former. This 
 hypothesis has derived much support from observations made in many 
 of the Lake Superior greenstone schists which are altered diabases. 
 In case of the particular rock under discussion, it is impossible to 
 prove with the material now in hand that the magnetite and associated 
 rutile have resulted from preexisting ilmenite, but in light of all that 
 we know of this and other occurrences, it seems to the w r riter that sucli 
 an origin is, to say the least, not at all improbable. Whether or not 
 such an alteration as that here suggested really takes place in the 
 ilmenite of diabase when this rock undergoes dynamic metamorphism 
 to chloritic schists must remain for future investigations to decide. 
 
 Eos. 4164 and 4105, from Prof. Irving’s collection, show the same 
 rock as the two specimens last described in a yet more advanced stage 
 of alteration. Both have become typical chlorite schists, composed 
 
 1 Allgomeino un<l chomischo Geologic, vol. 1, 1879, p. 97. 
 
102 
 
 GREENSTONE SCHIST AREAS OB' MICHIGAN. 
 
 [BULL- 62. 
 
 mostly of chlorite, quartz, and iron hydroxide. The structure is now 
 finely parallel and schistose, not the least trace of the original structure 
 remaining. In No. 4165, which is the darker colored of the two, leaf- 
 lets of a colorless mica (sericite) are abundant. 
 
 No. 11072, collected from Brooks’s point cc, is a dark green rock, which 
 is seen with the unaided eye to be traversed by numerous fibrous veins 
 of a paler green color. Under the microscope the section of this rock 
 shows principally ragged areas of green hornblende, inclosing isolated 
 crystals of a mineral, which agrees more closely in its physical proper- 
 ties with zoisite than with any other; i. e., there are colorless rectan- 
 gular sections with a cleavage parallel to the longest axis, and a cross- 
 parting in the direction perpendicular to this. In polarized light these 
 sections show pale, bluish gray interference colors, parallel extinction, 
 and a biaxial figure. The fibrous veins, which compose a considerable 
 proportion of the rock, are made up of zoisite individuals arranged 
 perpendicular to the walls of the vein, and of fibrous hornblende, which 
 often penetrates the former mineral in fine asbestiform needles. 
 
 THE LIGHT COLORED GREENSTONE AT UPPER QUINNESEC FALLS. 
 
 The speckled rock which forms the barrier at Dpper Quinnesec Falls, 
 is a very typical representative of the light colored greenstones of the 
 Menominee region. It has a strong macroscopical resemblance to the 
 rocks of this type already described from Sturgeon Falls and Lower 
 Quinnesec Falls, but is more attractive in appearance than any of them. 
 In the field it appears to be a medium grained aggregate of a white, 
 opaque feldspar, in which, however, glistening, striated surfaces are by 
 no means rare, and a grayish green mineral with a half metallic luster 
 on its cleavage planes. The deceptive appearance of this mineral is the 
 reason why Prof. Hermann Credner calls this rock (which he described 
 as early as 1870) a diabase with a decided resemblance to a gabbro. 1 
 
 This mineral does, indeed, show the most striking macroscopical sim- 
 ilarity to the diallage of some of the Volpersdorf and Italian gabbros; 
 but in spite of this fact, the most careful microscopical examination of 
 many different specimens — the freshest that could be discovered — 
 failed to disclose a trace of pyroxene. This result is the more surpris- 1 
 ing as the rock appears even fresher than that at Sturgeon Falls in 
 which considerable pale diallage still remains. The microscope, how- ; 
 ever, shows that the rock at Upper Quinnesec Falls is the more altered 4 
 of the two. 
 
 No. 11054, collected on the Wisconsin side of the river, directly at J 
 the fall, may be regarded as a typical specimen of the perfectly massive 3 
 
 1 In speaking of this constituent he says: “ Er [dor Augit] bihlet kurzsaukmfbrmige, zu krystal- a 
 linischeu Partion verwachsene Individuen, an dentin orthodiagoualo Spaltungstlachen mit halbme?^8 
 t allisohem Glanze besonders deutlich hervortreteu. Dadurch erhalt das Gestein eine Aehnlichkeit mit -S 
 Gabbro, selbst mit Hypersthonit.” (Neues Jahrbuch l'iir Mineral., 1870, p. 972.) Professor Pumpelly ; 1 
 also says tliat^kis rock is identical with that of Sturgeon Falls. (Geol. Wisconsin, Vol. 3, p. 564.) 
 
Williams.] GABBRO-DIORITE OF UPPER QUINNESEC FALLS. 
 
 103 
 
 rock. Its microscopical appearance is represented in Plate X, tig. 
 1. The hornblende is mostly of a very pale color and more or less 
 fibrous in structure. It has every appearance of being secondary, and yet 
 in every case where it can be traced into a more compact mineral this 
 is also a hornblende of a dark green or brown color. In many instances 
 the hornblende is bent and curved, as diullage is so apt to be (see right 
 side of the plate); but the most striking peculiarity of this hornblende 
 and the one most like diallage is its very perfect parting, parallel to the 
 orthopinacoid (100). This very unusual feature is apparently confined 
 to the paler, and probably secondary hornblende. It stops abruptly on 
 the edge of the compact, more deeply colored variety, even where this 
 is continuous with the lighter kind (Plate X, fig. I). 1 This may indi- 
 cate that the paler hornblende is secondary after diallage and therefore 
 reproduces its orthopinacoidal parting, while the diallage was itself 
 intergrown with an original compact hornblende which still remains. 
 Aside from its characteristic prismatic cleavage, proof is furnished that 
 this mineral is really hornblende by the fact that sections approximately 
 perpendicular to the vertical axis, give, in converged polarized light, a 
 bisectrix instead of an optical axis. 
 
 The feldspar of this rock is largely changed to opaque, gray saussur- 
 ite. Portions of it, however, remain in an unaltered state. These 
 have, even in the thinest sections, a pale brown color (PI. X, fig. 1), 
 and in thicker sections they are as dark as mahogany. This coloring 
 is not due to Inclusions from which the feldspar is surprisingly free, but 
 to some unevenly distributed pigment whose nature it is far beyond the 
 power of the microscope to reveal. With the exception of this color 
 the feldspar is so remarkably fresh and clear as to make the impression 
 at first glance that it must be of secondary origin. A slight examina- 
 tion, however, shows that the clear brown substance forms a peripheral 
 zone about the saussuritized individuals ; or where the whole crystal is 
 unchanged, that it is bent, broken, or faulted in a manner inconsistent 
 with any supposition of secondary origin. Here again we have addi- 
 tional, and, indeed, most convincing evidence that the greater the me- 
 chanical action to which the feldspar has been subjected, the less chem- 
 ical change it has undergone. (See above, p. 88.) 
 
 The other constituents of this rock are ilmenite, surrounded by a leu- 
 coxene border, and some secondary quartz, which is penetrated by most 
 delicate fibers of hornblende. 
 
 The analysis of this rock in column I of the following table was made 
 by Mr. B. B. Iiiggs: 
 
 1 It is interesting to note, in this connection, tho recent observation of Cathrein that the hornblende 
 of Roda in the Tyrol lias a perfectly developed parting due to very narrow twimiing-lamelhe which run 
 parallel to the orthopinacoid. (Zeitsclir. fur Kryst. u. Min., vol. 12, p. 12.) Whether tho above-men- 
 tioned parting is due to the same cause or not, it is impossible, on account of tho extreme narrowness 
 
 of the parting-liDes, to determine. 
 
104 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 . 
 
 1 i 
 
 ir. 
 
 j 
 
 Silica (Si0 2 ) 
 
 : 48.35 
 
 51.46 
 
 47.96 
 
 Alumina (A1 2 0 3 ) 
 
 15. 40 
 
 1 14. 35 
 
 I 16.85 
 
 Ferric oxide (Fe 2 0 3 ) 
 
 4. 04 
 
 3/90 
 
 : 4.33 
 
 Ferrous oxide (FeO)..-. - 
 
 4.63 
 
 5.28 
 
 ' 4.17 
 
 Lime(CaO) 
 
 10. 38 
 
 9. 08 
 
 13. 25 
 
 Magnesia (MgO) 
 
 11.61 
 
 9. 54 
 
 9.15 
 
 Soda (Xa. 2 0) .’. 
 
 1.87 
 
 2. 92 
 
 1.25 
 
 .Potasli (K a O) 
 
 • 35 
 
 .24 
 
 .30 
 
 Water (H 2 0) 
 
 3.60 
 
 3. 30 
 
 2. 89 
 
 Carbon dioxide (C0 2 ) . . . 
 
 .08 
 
 .20 
 
 .08 
 
 Total 
 
 100.31 
 
 100. 27 
 
 ! 100.23 
 
 Dried at 105°. 
 
 The analyses of the two analogous rocks, Nos. 11171 (II) from Sturgeon 
 Falls, and 11008 (III), from Lower Quinnesec Falls, are again cited from 
 pp. 76 and 89, for comparison. The agreement between all three analyses 
 is as close as could be expected for three different specimens of the 
 same rockmass. In fact it is difficult to escape the conviction that the 
 rocks from both Upper and Lower Quinnesec Falls, like that from Stur- 
 geon Falls, were once diallage-plagioclase aggregates or gabbros $ and 
 yet if this be true, we are compelled to assume either that the original 
 diallage passed by paramorphism into compact brown hornblende be- 
 fore reaching its present state ; or that the original rock was a horn- 
 blende gabbro in which both bisilicate constituents passed finally into 
 pale fibrous hornblende, although this process progressed much more 
 slowly with the hornblende than with the pyroxene. 
 
 The feldspathic component of this rock (No. 11054) is determined by 
 the analysis to be labradorite, as was also found to be the case in the 
 corresponding specimens from the other localities. 
 
 Two other specimens of this same rock, No. 11061, from the Michi- 
 gan side of the falls, and No. 11073, from a point above the falls, 
 marked p on Major Brooks’s map, are essentially the same as the one 
 just described. Both are, however, more altered and both show, in a 
 still greater degree, the effects of pressure upon the constituent minerals. 
 In No. 11061 a good deal of quartz is present, always penetrated by 
 delicate needles and tufts of hornblende. The largest areas of this 
 quartz form a rather coarse grained mosaic and look as though they 
 had been deposited as a pseudomorph after some former constituent. 
 Some colorless chlorite is also present in this section, having been de- 
 rived from the alteration of the hornblende. The feldspar of No. 
 11073 is colorless, and has been fissured, broken, and even crushed in a 
 surprising manner. As a result, the saussuritization of this mineral has 
 hardly more than commenced, in spite of the advanced state of altera- 
 tion observable in the hornblende. One hornblende section in this 
 slide, cut nearly perpendicular to the vertical axis, shows a very sharp 
 line of demarcation between the interior, dark brown portion and the 
 
wiluams.] SHEARED GABBRO-DIORITE. 105 
 
 colorless peripheral zone. This resembles somewhat the secondary horn- 
 blende enlargements recently described by Van Hise, 1 but I can not 
 regard this particular case as due to anything but exterior bleaching. 
 
 Nos. 11056 and 11057, from the Wisconsin side of the fall, illustrate 
 the passage of this pale diorite into schistose varieties, as described at 
 Lower Quinnesec Falls. The former specimen, though macroscopicaily 
 still quite massite, has lost the distinctness of its structure. Under the 
 microscope this is seen to be due to crushing and attendant chemical 
 changes. The feldspar is almost pulverized, but has otherwise un- 
 dergone but little change. A few of the larger crystals have been merely 
 
 cracked and faulted as shown in Fig. 
 11. The hornblende is very largely 
 changed to a colorless chlorite. 
 Where one of the hornblende crys- 
 tals has been broken and sheared, 
 chlorite is seen to have been devel- 
 oped in parallel fibers. This fur- 
 nishes an admirable microscopic illus- 
 tration of how the schistose bands 
 are formed by pressure in the rock- 
 mass as a whole. (See also Fig. 22, p. 
 128.) Just below the falls this rock 
 becomes broken, gashed, and seamed 
 with narrow, paraliel veins of lamel- 
 lar minerals. These gradually in- 
 crease to bands, which finally com- 
 pose the main portion of the rock. There can remain no doubt in the 
 mind of anyone who will carefully study this exposure, that these schis- 
 tose bands have been produced in the massive rock by the action of 
 pressure, along lines where there has been a shearing motion. 
 
 No. 11057 is from one of the schistose bands in No. 11056. The micro- 
 scope shows it to be composed of a fine mosaic of quartz and feldspar (?) 
 grains, made schistose by parallel fibers of serpentine and chlorite. 
 
 At and just below the engine house on the Michigan side of Upper 
 Quinnesec. Falls is another exposure which illustrates the gradual 
 passage of these light colored, massive greenstones, into silvery, hydrous 
 schists, similar to those described as occurring just below Lower Quin- 
 nesec Falls. 
 
 No. 11065 is a very light colored, although nearly massive, rock, seen 
 in situ in a wall behind the engine house. It is composed of much 
 crushed and faulted feldspar of the above described brown variety, 
 together with colorless isotropic chlorite. There is also some of the 
 quartz albite mosaic, though this is not abundantly developed, with a 
 little iron oxide. There is no parallelism in the arrangement of the 
 constituents which would tend to produce a schistose structure. 
 
 Fig. 11. — Faulted feldspar crystal in crushed 
 greenstone (No. 11056) from Upper Quinnesec 
 Falls. Nicols crossed ; magnified 30 diame- 
 ters. 
 
 1 Am. Jour. Sci., 3d series vol., 33, 1887, p. 385. 
 
106 GREENSTONE SCHIST AREAS OF MICHIGAN. [bul'l. 62 . 
 
 No. HOGG is from the same rock- wall as the last specimen and is un- 
 doubtedly continuous with it. It is decidedly schistose, and is com- 
 posed wholly of a granular mosaic, with both sericite scales and a col- 
 orless chlorite. There are the finest microscopic rutile crystals in this 
 
 rock that were encountered in any 
 specim ens from the Menominee region . 
 These crystals are simple individuals, 
 twins and trillings showing a great 
 variety of form. A few are repre- 
 sented in the accompanying figure. 
 They are grouped together or ar- 
 ranged in lines or strings which fol- 
 low the direction of the schistosity. 
 As in other similar instances before 
 described from the Lower Falls, they 
 appear to have originated from the 
 alteration of the ilmenite of the mas- 
 sive rock. 
 
 Just below the engine-house similar 
 sericite schists are exposed (No. 11067 ] ) which contain green chlorite in 
 spots and appear to grade into typical dark green chlorite schists (No. 
 11068). These rocks are mentioned by Major Brooks at the exposures 
 marked on his map x and y 2 . These dark green schists are like those 
 which originate from the alteration of the dark colored diabases, and 
 their appearance probably marks the commencement of the belt of these 
 rocks which skirts the basin below the Falls. 
 
 Fig. 12.— Ru tile needles in Xo. 71056 magnified 
 350 diameters. 
 
 THE COARSE GRAINED DIORITES OF THE HORSE RACE. 
 
 The half mile of comparatively quiet water, navigable by a small 
 boat or canoe, immediately above the tJ pper Quinnesec Falls is bordered 
 mostly by massive or schistose greenstones of the dark type similar in 
 all respects to the rocks of this kind which have been studied at sev- 
 eral other localities on the Menominee River. They are interspersed 
 with bands of gneissose rock, identical with those yet to be de- 
 scribed. 
 
 The narrow gorge known as the Horse Race, through which the river 
 flows for a mile or more, has, however, been excavated through rocks 
 of a quite different character. These are for the most part coarse 
 grained diorites, penetrated by bands of granitic and gneissic rocks 
 which will receive special consideration in the following section. 
 
 Typical specimens of these coarse grained diorites are Nos. 11077 and 
 11093 from the Wisconsin, and Nos. 11182, 11183, 11185, aud 11186 
 from the Michigan side of the rapids. 
 
 The macroscopical appearance of these rocks is often that of an almost 
 
 ‘This rock was called by H. Credner “ talc-schist ” in 1869 (Zeitschr. Deutsch. geol. Gesell., vol. 
 21, p. 529). It was described in 1876 by Wichmann, who gives seven reasons for regarding the sericite 
 schists as of fragmental origin. (Geol. Wisconsin, vol. 3, p. 638.) 
 
 2 Ibid., 1, pp. 473,474. 
 
 
 
 
 
williams.] THE DIORITES OF THE “ HORSE RACE.” 107 
 
 uniformly gray mass, in which the large and frequently glistening horn- 
 blende crystals are not at first glance very apparent. This color is due 
 to the alteration of the feldspar, in which new minerals are largely de- 
 veloped. An opaque, while feldspar, or rather saussurite, is, however, 
 often visible. This is sometimes in the form of rounded or oval areas 
 which represent the centers of crystals that have turned gray around 
 their edges ; sometimes in the form of the original feldspar crystals 
 themselves, and agaiu in sharp contrast with the dark green horn- 
 blende. The grain of these rocks varies extremely, but is rarely fine. 
 The form of the different constituents is always visible to the naked 
 eye ; and, in some instances (No. 11192), these measure from one to 
 two inches in diameter. 
 
 Aside from the unusual coarseness of their grain, the rocks of the 
 Horse Race differ from the other greenstones of the Menominee in fre- 
 quently containing biotite. Another striking contrast is presented in 
 the almost universal presence of talc. This mineral has without 
 doubt originated from the hornblende, and has wandered from it 
 into the feldspar. It is scattered everywhere through the rock in 
 minute, silvery, glistening scales, and it coats all cracks and fissures. 
 The surface of the hornblende crystals is also frequently spotted with 
 it. The nature of this mineral as talc is easily determined by both op- 
 tical and chemical means. Under the microscope it is of a pale green 
 color, resembling muscovite in its cleavage and brilliant interference 
 colors, but with a small optical angle and negative character. It is 
 infusible and not attacked by acids, while microchemical tests show 
 that it is destitute of both alumina and alkalies. 
 
 The structure of the Horse Race rocks is that of the second kind 
 mentioned by Rosenbusch as occurring in diorite, 1 i. e., that conditioned 
 by the feldspar having crystallized before the hornblende. The latter 
 component is plainly allotrimorphic, like the pyroxene in diabase, 
 while the feldspar has a well developed form of its own. (PI. XII, 
 fig. 2.) The hornblende, although comparatively compact and homo- 
 geneous over considerable areas, nevertheless conveys the impression 
 of being of secondary origin. It has a pale green color, slightly darker 
 toward the edge, and is externally frayed out into a fringe of radiat- 
 ing actinolite fibers, which wander along the cracks in the feldspar. 
 (No. 11186; see PI. XII, fig. 2.) In some sections — notably in No. 
 11185 — large portions of the hornblende have become wholly changed 
 to a felt like network of minute fibers. These characters, together 
 with the shape of the hornblende individuals, convey the impression 
 that they have been derived from pyroxene. While, therefore, it is 
 impossible to prove it with certainty, it is difficult to escape the con- 
 viction that these rocks were originally coarse grained gabbros or 
 diabases. 
 
 The feldspar shows in almost every instance a broad twinning stria- 
 
 Mikroa. Physiog., 2d cd., vol.2, p. 121. 
 
108 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62 . 
 
 tioii, although this is more or less obscured by chemical changes. In 
 one specimen (No. 11182) there is a brown feldspar which is perfectly 
 preserved around the periphery of the crystals, while their interior is 
 changed to saussurite. In other cases (Nos. 11093 and 11185) the feld- 
 spar is largely changed to saussurite, with which is mingled a good deal of 
 actiuolite and some biotite. In the latter case clear areas of brilliantly 
 polarizing talc are quite abundant. In Nos. 11077 and 11186 the white 
 or colorless feldspar is comparatively well preserved, but it is filled with 
 pale green actinolite needles and some little biotite, which appear to 
 have wandered into it from the hornblende. In these rocks the amount 
 of saussurite is inconsiderable. 
 
 Brown biotite is not infrequently an important constituent of these 
 rocks. It is especially abundant in No. 11077. Although sparingly 
 scattered through the feldspar like the actinolite, it is mainly to be 
 found in close association with the hornblende, with which or out of 
 which it seems to have been developed by secondary processes. 
 
 Other specimens represent exceptional varieties of the Horse Bace 
 diorites. 
 
 No. 11091, from the Wisconsin bank of the stream, shows the feld- 
 spar wholly changed to a compact aggregate of epidote grains. 1 The 
 hornblende, which is in sharp crystals, presents its usual appearance 
 and characteristics. The epidote is so light colored that it might 
 easily be mistaken at first glance for feldspar in the hand-specimen. 
 The microscope, however, at once shows its true character. The inter- 
 ference colors of the closely interlocking grains present a brilliant 
 appearance. No trace of the original feldspar remains. Only an occa- 
 sional grain of calcite or quartz interrupts the continuity of the epidote. 
 Epidote is not an unusual secondary product in feldspar, although such 
 perfect pseudomorphs of this mineral as are here present are rare. 2 
 
 Still other specimens show, in a marked degree, the effects of dy- 
 namic metamorphism upon the Horse Bace rocks. No, 11189, from the 
 head of the rapid, on the Michigan side, has a pronounced gneissic 
 structure. Its hornblende is of the usual character, sometimes in com- 
 pact crystalloids of large size, sometimes in a fibrous aggregate, but 
 almost always much twisted, bent, or broken. The feldspar, in some 
 instances, is completely changed to an aggregate of epidote crystals, as 
 in the rock last described ; in others, it merely has minute, highly re- 
 fracting epidote grains more or less abundantly developed in it (saus- 
 snritization). These are often accompanied by rhombic dodecahedra 
 of a colorless garnet. 3 Other of the feldspar individuals show a me- 
 chanical rather than a chemical alteration. There is, in some cases, a 
 
 1 A not unusual alteration according to Rotli ; Allgemeine nnd chemisclie Geologie, vol. 1, 1879, p. 32l. 
 
 2 Cohen mentions such a perfect transformation of feldspar to epidote in the diorite which forms the 
 base of the island Palma. Neues Jahrbuch fiir Mineral., 1876, p. 751. Rosenbuseh also mentions them 
 in diorites from the Vosges Mountains. Mikros. Physiog., 2d ed., vol. 2, p. 103. 
 
 3 Rosenbuseh: Mikros. Physiog., 2d ed., vol. 2, p. 136. Paul Michael finds one of the two varie- 
 ties of saussurite in the gabbro of Wojaleite, Fichtelgebirge, composed of a lime-alumina garnet and 
 serpentine. Neues Jahrbuch fiir Mineral., 1888, vol. 1, p. 39. 
 
williams. 1 THE DIORITES OF THE “ HORSE RACE. 77 109 
 
 peripheral granulation (ranclliche kataklase) producing the “ mortar 
 structure 77 (Mdrtel-Structur of Tornebohm). In other cases there is a 
 complete reduction of the whole feldspar crystal to a granular mosaic, 
 while in still others there is only a separation into large, interlocking, 
 and but slightly disturbed areas. Fine veins of epidote not infrequently 
 traverse these feldspar crystals. A jioint of mineralogical importance 
 connected with this rock is the evidence it affords of the alteration of 
 ilmenite into sphene. The usual alteration product of this mineral, 
 leucoxene, is now generally believed to belong to this species, but it is 
 rare to find the crystalline form of the sphene so typically developed as 
 in this section. The mineral is of a grayish brown color and nearly 
 opaque, like the secondary leucoxene which surrounds ilmenite. It 
 polarizes with dull colors, but there is no mistaking its nature on ac- 
 count of its characteristic form. (PI. XIII, fig. I.) 1 
 
 No. 11078, collected on the Wisconsin side of the river, just below 
 the Horse Eace, is perfectly continuous with No. 11077, above described, 
 and represents a phase of this rock produced by the action of intense 
 pressure. The hornblende is almost wholly changed to an aggregate 
 of weakly polarizing fibers, which, according to the descriptions of 
 Eosenbusch, are perhaps best regarded as of a serpentinous nature. 
 These twine in and around the feldspar so as to produce a sort of 
 “ Flaser 77 structure. The feldspars themselves are sometimes reduced to 
 a mosaic ; but sometimes they have only a peripheral granulation. Much 
 of the biotite of the unaltered rock remains among the alteration prod- 
 ucts of the hornblende. The iron ore has been drawn out into sinuous 
 stringers which follow the direction of the foliation. 
 
 No. 11191 was taken from a wavy schistose, chloritic band on the 
 Michigan side of the Horse Eace. It has a strike 30° E. of N., and 
 traverses a coarse grained massive greenstone, into which it passes by 
 insensible gradations. In this rock there is considerable hornblende, 
 which is seen in the process of transformation to a fibrous, yellow ser- 
 pentine. The feldspar is of the reddish brown variety and has under- 
 gone granulation around the edge. This has been accompanied by the 
 production of quartz and calcite. In a large area of the latter mineral 
 there are crystals of a substance whose exact nature could not be de- 
 termined, It has the bluish interference colors of zoisite, a parallel 
 extinction and a biaxial interference figure. It is also changing to the 
 same yellow serpentine as the hornblende. The sepentiue penetrates 
 and traverses it as it does crystals of olivine. Chlorite is also a frequent 
 component of this rock. 
 
 Nos. 11080 and 11195 are exceptionally fine grained greenstones, the 
 former from the foot and the latter from the head of the Horse Eace. 
 Both are composed essentially of actinolite, feldspar, quartz, and epi- 
 dote, and resemble in their microscopical appearance and structure the 
 
 1 Schonck observed tho titanic iron entirely replaced by sphene in a schistose diabase from the 
 upper Buhr Valley. Inaugural Dissertation, Bonn, 1884, p. 57. 
 
110 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 typical so-called “ crystalline schists.” Still the former is massive and 
 cuts across the strike of schistose rocks like a dike, while the latter is 
 decidedly schistose. No. 11195 contains minute and sharp, dark brown 
 sphene crystals, which appear to have originated, like those in No. 
 11? 89, from the alteration of ilmenite. 
 
 THE ACID ROCKS OF UPPER QUINNESEC FALLS AND THE HORSE RACE. 
 
 Among the rocks to be found in the neighborhood of the Upper Quin- 
 nesec Falls and Horse Race are those of an acid type. They occur in 
 bands of varying width, which generally, but not always, conform to 
 the foliation of the greenstones. These acid rocks are sometimes mass- 
 ive granites without a trace of schistose structure ; sometimes gneisses 
 with a “Flaser” or “Augen” structure, and sometimes finely banded and 
 schistose rocks like the Saxon granulites. Whenever these bands show 
 any indications of schistose structure this seems to be conformable to 
 the cleavage of the adjoining greenstones, without reference to what 
 the direction of the band itself may be. Inasmuch, however, as these 
 two directions generally coincide, it is not common that the foliation of 
 the acid bands makes any angle with their sides. Such instances were 
 nevertheless occasionally found, and they have a very important bear- 
 ing on the genesis of these rocks and on their relation to the green- 
 stones which surround them. 
 
 An inspection of the published geological maps of the region south 
 of Lake Superior 1 will show that immediately south of the portion of 
 the Menominee River under discussion there is an enormous area of a 
 typical granite. Major Brooks, in his report on the Menominee dis- 
 trict, thinks that this granite may very possibly be of eruptive origin, 
 but, whether so or not, that it certainly overlies and penetrates (“in 
 veins”) the upper members of the greenstone series. 2 Since, however, 
 he regards the greenstones as occupying the upper portion of the Hu- 
 ronian formation, he is compelled to assume that the granite represents 
 its youngest member and hence he designates it as the “Huronian 
 granite.” (See profile, Fig. 2.) 
 
 Without entering in this place into a discussion of the stratigraphical 
 relationships of these rocks, it may at least be stated with certainty 
 that this granite does penetrate the greenstones in the form of dikes 
 and apophyses, especially where the main mass approaches nearest to 
 the river. This point is about half a mile south of the Horse Race, as 
 may be seen by Major Brooks’s section and map of this region 3 . Here 
 the typical, coarse grained and somewhat porphyritic granite appears 
 in a high ridge. 
 
 The adjacent greenstones and greenstone schists do not here materi- 
 ally differ from those at Upper Quinnesec Falls. They strike nearly east 
 
 1 Geol. Wisconsin, vol. 3, atlas, FI. XXVIII; Mon. U. S. Geol. Survey, vol. 5, PI. I ; Fifth Ann. 
 
 Kept. U. S. Geol. Survoy, FI. XXII. 
 
 2 Geol. Wisconsin, vol. 3, pp. 452, 531, 719. 3 Ibid., PI. Ill, p. 472. 
 
WILLIAMS. 1 GRANITE SOUTH OF THE u HORSE RACE. ” 111 
 
 and west and dip to the south. Near the granite contact they are filled 
 with dikes of all sizes, evidently offshoots from the main granite mass 
 (Nos. 11105 to 11107). These dikes, when small, are fine grained and 
 felsitic, but when larger their texture is coarser and they have fre- 
 quently a well developed schistose structure parallel to that of the ad- 
 joining schists. After a careful examination of this locality and of the 
 exposures between it and the river, there is no .doubt in the writer’s 
 mind that the granite, u Augengneiss,” biotitic gneiss, and schistose 
 porphyry (or u por phyroid,” as Credner calls this rock) visible near the 
 Upper Quinnesec Falls and along the Horse Bace, are also dikes or 
 aphophyses connected with the main southern granite area. The schis- 
 tose or banded structure of these rocks, when such exists, is a secondary 
 feature, produced by the same dynamic agencies which rendered the 
 greenstones themselves schistose. 
 
 An intelligent study of these acid rocks should begin with an exami- 
 nation of the massive granite from the large area south of the Menominee. 
 No. 11104 was collected near the contact, about half a mile south of the 
 Horse Bace, where, after appearing in numerous dikes in the green- 
 stone, the solid mass of granite appears in an abrupt wall, trending N. 
 80° E. This rock appears in a hand-specimen to be a typical, coarse 
 grained granitite, with a decided tendency to a porphyritic structure. 
 The latter feature may, however, be due to the nearness of this locality 
 to the contact. When examined under the microscope, the macroscopic 
 diagnosis is found to be correct and several additional points of interest 
 are brought to light. The oldest constituents are zircon and apatite; 
 both quite abundant in the form usual in granitic rocks. Iron oxide 
 seems to be almost absent as an original constituent, though it is found 
 in some of the altered micas. The biotite, the only mica present, is not 
 abundant. It is invariably bleached to a green color by the reduction 
 of its iron to the ferrous state. It contains abundant inclusions of apa- 
 tite, zircon (around which are pleochroic aureoles), and some secondary 
 magnetite. No trace of either hornblende or pyroxene was observed. 
 Sphene, however, is present, as are also a few sharp crystals of a dark 
 grayish blue tourmaline. The principal interest of this rock attaches to 
 its feldspar and quartz. They together make up nearly the whole mass 
 and exhibit, in a remarkable degree, the effects of pressure. The feldspar 
 is of three kinds : normal plagioclase (oligoclase), unstriated orthoclase, 
 and inicrocline. The relationship of these species of feldspar is a sug- 
 gestive one. Both the oligoclase and the orthoclase are always altered 
 to a fine micaceous or kaolinitic product which is particularly abundant 
 in the center of the crystals, a zone of the unaltered mineral being often 
 preserved around the edge. The microcline, on the other hand, almost 
 never shows any indication of alteration. 
 
 It is always clear and fresh in appearance, but its twinning lamellae 
 are bent or curved and bear every sign of having been secondarily de- 
 veloped. 1 In other words, we have here again, in the writer’s opinion, 
 
 •Rosenbnsc.h, Mikros. Phyaiog., 2d ed., vol. 2, p. 295. 
 
112 
 
 GREENSTONE SCHIST AREAS OE MICHIGAN. 
 
 [BULL. 62. 
 
 a striking example of the mechanical action apparent in the feldspar, be- 
 ing inversely proportional to the chemical action which has gone on in it. 
 Original orthoclase has been converted partly into kaolin, partly into 
 microeline, according to the way in which the action of the force mani- 
 fested itself. The effect of the force which acted upon this rock is also 
 apparent in other ways. The large original feldspar crystals show a 
 peripheral granulation (see Chapter I, p. 49), and where they have been 
 fissured their cracks are filled with a new crystallization of plagioclase, 
 orthoclase, and quartz. None of these minerals shows any signs of 
 chemical alteration and microeline is never to be found among them. 
 Thus is produced a good example of what Tornebohm has called a mor- 
 tar structure (“Mortel-Structur”) 1 . In this secondary cement-like ag- 
 gregate, a micropegmatitic intergrowth of quartz and feldspar is quite 
 common, and calcite, in good-sized Individuals, is by no means rare. 
 
 The original quartz of this granite also shows many indications of 
 having been squeezed. The crystals or grains often have an undulatory 
 extinction, Avhile larger grains are broken and the fragments are more 
 or less displaced. Proof that these were not originally different grains is 
 given in section No. 11104, where a small tourmaline crystal is broken 
 
 (See Fig. 13). No. 11105 is a speci- 
 men of the prevailing rock near the 
 granite contact. This is a horn blende 
 schist, composed mainly of irregular 
 grains of dark green hornblende and 
 quartz. There are beside some stri- 
 ated and some unstriated feldspars, 
 a little sphene and an abundance of 
 extremely sharp and clear epidote 
 crystals. The banding of this rock 
 is caused by the preponderance of 
 hornblende in some layers and of 
 quartz in others. Its strike is nearly 
 east and west and its dip 75° to 
 80° to the south. Under the micro- 
 scope all of the constituents by 
 their extreme freshness and freedom 
 from all inclusions convey the impression of being secondary crystal- 
 lizations. The texture of the rock is granular, although the epidote 
 is present either in exceedingly sharp crystals (which often pass 
 unbroken from one quartz grain into another) or in much more 
 minute, ovoid granules, forming the little, highly refracting particles 
 which are so common in the crystalline schists. No. 11107 was 
 taken from one of the wider of the numerous acid dikes which pene- 
 
 1 N&,gra oid om granit ocli gneis. Geol. Foren. Stockholm Forhandl., 1880-’81, vol. 5, p. 233, (ref. 
 Neues Jahrbuch fur Mineral., 1881, vol. 2, Referate, p. 51; and Roseubuscb, Mikros. Pkysiog., 2d ed., 
 vol. 2, p. 42.) 
 
 2 Compare Dr. Chelius’s remarks on the Hessian granite-porphyries, Notizblatt des Vereius fur Erd- 
 kunde zu Darmstadt, 1883. 
 
 and faulted just at the contact. 2 
 
 Fig. 13.— Broken tourmaline crystal proving 
 the secondary fracture of the inclosing quartz 
 grain, “Horse Race” granite. No. 11104. 
 
WILLIAMS.] 
 
 GRANITE GNEISSES OF THE “ HORSE RACE.” 
 
 113 
 
 trate the last described hornblende schist in the neighborhood of the 
 granite contact. It has a decidedly gneissic structure parallel to the 
 banding of the inclosing schist, which is here also the direction of this 
 band or dike. The microscope shows that the mineral composition of 
 this rock is identical with that of the coarse granite (No. 11104). 
 There is the same zircon, sphene, and tourmaline associated with the 
 biotite, feldspar, and quartz. The differences are the gneissic structure, 
 fineness of grain and absence of all porphyritic structure in the dike 
 rock, while none of its constituent minerals show the chemical altera- 
 tion which has progressed so far in the massive granite. Both the 
 biotite and the feldspar are quite fresh, the rich brown color of the for- 
 mer contrasting with green and bleached mica above described. 
 
 After the foregoing review of the character of the acid rocks at and 
 near the granite contact, we are in a much better condition to under- 
 stand the occurrence of the bands of gneiss and porphyroid near the 
 Upper Quinnesec Falls, which were observed by Major Brooks and Prof. 
 Pumpelly. 1 If we now examine some of the most typical of these ex- 
 posures with care, we shall find that they are quite identical with the 
 rocks which we have just been considering. 
 
 On the lower side of a small cove which indents the Wisconsin 
 river bank immediately below the Horse Race there is a narrow band 
 of acid rock well exposed on the shore. The center of this band is com- 
 posed of a massive, gray colored, porphyritic rock resembling a granite 
 (No. 11082). This grades on both sides imperceptibly into a well char- 
 acterized, fine grained gneiss (No. 11085), which in places is so finely 
 banded as to resemble some of the Saxon granulites (No. 11084). The 
 foliation of this exposure is nearly vertical and seems to be quite par- 
 allel to the sides of the band, which itself makes only a slight angle with 
 the cleavage of the adjoining greenstones. 
 
 No. 11082 was collected from the central and most massive portion 
 of this acid band. Macroscopically the rock appears to be a typical 
 granite porphyry, nor does the examination of a thin section with the 
 microscope reveal anything opposed to this determination. The follow- 
 ing analysis of the. rock, however, made by Mr. R. B. Riggs, shows that 
 this rock is in reality a diorite : 
 
 Silica (Si0 2 ) 
 
 Alumina (A1 2 0 ;5 ) 
 
 Ferric oxide (Fe 2 0 ;j ) . 
 Ferrous oxide (FeO) . 
 
 Lime (CaO) 
 
 Magnesia (MgO) 
 
 Soda (Na 2 0) 
 
 Potash (KjO) 
 
 Water (H 2 0) 
 
 Carbou dioxide (CO.) 
 
 54.83 
 25. 49 
 1.61 
 1. 65 
 6. 08 
 1.96 
 5. 69 
 1.87 
 1.18 
 .18 
 
 Total 
 
 100. 54 
 
 Bull. 02 8 
 
 Gool. Wisconsin, vol. 3, p. 474, 
 
114 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62. 
 
 The microscope discloses good-sized crystals of a striated and zonally 
 formed feldspar embedded in a granular mosaic of clear, colorless, and 
 unstriated grains associated with brown leaflet of biotite. Apatite, 
 zircon, and a reddish pleochroic sphene are also present in small crys- 
 tals. . In spite of this rock showing no indication whatever of altera- 
 tion, it contains calcite in considerable quantity. This mineral appar- 
 ently penetrates and includes all the other constituents in a manner 
 which has led Hawes, 1 Tornebohm, 2 and Chrustsclioff, 3 to regard it 
 under similar circumstances as a product of the original crystallization. 
 
 In one section of the present rock sharply defined sphene crystals were 
 observed wholly surrounded by the calcite. Nevertheless the presence 
 of this carbonate in the fresh rock is to be explained, as Rosenbusch 
 suggests, by the filling up of drusy or miarolitic cavities. 4 
 
 The rock appears both raacroscopically and microscopically to be a 
 granite porphyry with a microgranitic groundmass. The analysis, how- 
 ever, shows it to be largely composed of a feldspar of the andesine 
 series, and this is also indicated by a further examination. The color- 
 less grains of the groundmass, in spite of their limpid character and 
 superficial resemblance to quartz, give in converged polarized light the 
 brush or hyperbola of a biaxial crystal. In the Thoulet solution the 
 colorless portion 6f the powder fell between 2.683 and 2.650, a large 
 proportion, however, being confined between the limits 2.668 and 2.659. 
 
 A small proportion possessed exactly the specific gravity of quartz, 
 so that it is impossible to say with certainty whether this mineral is 
 present in the groundmass. The relative proportions of silica and 
 alumina, however, as given by the analysis, make this improbable. We 
 must describe this rock as a very pure type of a mica-diorite porphyry ; 
 whose groundmass is composed of a mosaic of clear unstriated lime- 
 soda feldspar, probably andesine. 
 
 The two specimens (Nos. 11084 and 11085), taken from the gneissic 
 portion of this exposure, when seen under the microscope, closely re- 
 semble the groundmass of the diorite porphyry just described. The 
 chief difference is in the banded appearance, produced by the parallel 
 arrangement of the grains, and especially of the mica x>lates. This is 
 most pronounced in No. 11084, where the mica is collected in certain 
 layers and where there is also an alternation in the grain, some layers 
 being coarser and others finer. Occasional tourmaline crystals are 
 here associated with the zircon and apatite. Calcite also is present, as 
 in the last described rock, but now it is in stringers and arranged, like 
 all the other components, in the direction of the schistosity. No. 11085 
 has neither the calcite nor the tourmaline. Its most interesting feature 
 is the presence of long strings of minute rutile crystals which appear to 
 
 1 Geology ot New Hampshire, vol. 3, Part IV : Mineralogy and Lithology, 1878, p. 208, PI. XII, Fig. 1.. { 
 
 2 0m Kalkgranit. Geol. Fdceu Stockholm Forhandh, vol. 3, 1876, p. 210. Om Kalcithalti graniter. 
 Kong. Vetensk. ak. Fdrhandl., vol. 5, 1881, p. 233. 
 
 3 Bull. Soe. Mineral, de France, vol. 8, 1885, p. 137. 
 
 4 Mikros. Physiog., 2d ed., vol. 2, 1885, p. 34. 
 
WILLIAMS.] 
 
 GRANITE GNEISSES OF THE u HORSE RACE.” 115 
 
 have originated from the alteration of the biotite. No. 11079, collected 
 from a narrow acid band slightly east of this exposure, is quite ident- 
 ical in both composition and structure with the two last mentioned 
 rocks. There are here occasional re- 
 mains of former porphyritic feldspar 
 crystals which have been mostly de- 
 stroyed by granulation. Tourmaline 
 is quite abundant, as are also flakes of 
 colorless but brightly polarizing sericite. 
 
 It will be seen that these rocks are 
 quite the same as those found farther 
 south at the granite contact. Along 
 the whole extent of the Horse Race 
 similar acid rocks are very abundant. 
 
 They occur in bands varying from the 
 finest seams to such as are many yards 
 in width. While these as a rule follow 
 the direction of the foliation of the 
 greenstones, they by no means always 
 do so. Their mode of occurrence often 
 bears strong testimony to their intru- 
 sive nature, as may be seen from the 
 following figures sketched at the head 
 of the Horse Race on the Michigan side 
 of the river. 
 
 Fig. 14 shows two bands of gneiss, one parallel to the strike of the 
 greenstones, the other cutting across it. Iu each the lamination of the 
 acid rock coincides with that of the greenstones, without regard to the 
 sides of the band. This would seem conclusive evidence of the second- 
 ary nature of the gneissic structure. 
 
 cove at tlic head of the Horse Race. Direc- 
 tion of the shading lines indicates the 
 strike. 
 
 Fig. 15. — Foliated granite (gneiss) intrusive in greenstone. Head of the Horse Race. 
 
 Fig. 15 shows a band of gneiss which comes to an abrupt termina- 
 tion in the greenstone and which sends out apophyses into this, as only 
 an intrusive dike would do. 
 
116 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN, 
 
 [BULL. 62 . 
 
 Fig. 16 shows an irregular area of gneiss penetrating the greenstone. 
 The lines in the drawing indicate the direction of the foliation. This 
 may be a cross-section of a laterally intrusive arm. 
 
 Fig. 16 .— Foliated granite (gneiss) intrusive in greenstone. Head of the Horse Race. 
 
 Many other exposures might be selected to prove the intrusive 
 nature of these acid rocks at the Upper Quinnesec Falls, but the oues 
 already cited will suffice for the present purpose. 
 
 With respect to their structure, the acid rocks of the Upper Quin- 
 nesec Falls and Horse Race may be classified as follows : 
 
 I. Porphyntic: 
 
 Granite porphyry, represented by Nos. 11104, 11082, 11087, 
 11089, 11190. 
 
 Augen-Gneiss, represented by Nos. 11184, 11193 11196. 
 
 Schistose porphyry, represented by Nos. 11050, 11051, 11052, 
 11096. 
 
 II. Non-porphyritic : 
 
 Gneiss, represented by Nos. 11079, 11084, 11085, 11188. 
 
 Felsite, represented by No, 11071. 
 
 The main points of interest will now be stated with reference to each 
 of these types in succession, although no further mention will be made 
 of those specimens which have already been described, viz, Nos. 11104, 
 11082, 11084, 11085, 11079. 
 
 It is believed that the distinctive features of the schistose and 
 banded rocks of this region have to a great extent been produced by 
 secondary causes. An original porpliyritic structure seems to have been 
 very prevalent, if not universal, in all of these acid dikes. We are able 
 to trace its gradual disappearance, and we find that this is proportional 
 to the intensity of the dynamic action to which the particular rock has 
 been subjected. The crushing or rubbing of the constituent minerals 
 against one another has produced a peripheral granulation ( u randliclie 
 Kataklase”). This has altered the porpliyritic crystals into the eyes 
 or “Augen” of the' gneisses and schistose porphyries, as is shown in 
 PI. XV, fig. 1 ; and there seems no reason why its extreme applica- 
 tion may not have changed a porpliyritic rock to a felsite. 
 
WILLIAMS.] 
 
 ORTHITE IN GRANITE. 
 
 117 
 
 Granite porphyry. — No. 11190, from the Michigan side of the Horse 
 Race, near its center, is from a small area of acid rock exposed at the 
 water’s edge, which seems to be completely surrounded on the three 
 other sides by diorite. It is porphyritic, bat contains a very large pro- 
 portion of feldspars (mostly striated) and comparatively little ground - 
 mass. This latter is so arranged as to produce a resemblance to the 
 mortar -structure, and thus the rock approaches No. 11101, although all 
 of its quartz is confined to the groundmass. Biotite is quite abundant. 
 It contains fine pleochroic aureoles, and is frequently bleached to a 
 pale green color. 
 
 Nos. 11087 and 11089, both from the Wisconsin bank of the Horse 
 Race, are decidedly porphyritic. A fine grained granular groundmass 
 is in sharp contrast to the well formed feldspar crystals. These are 
 noticeable on account of their finely developed zonal structure, which 
 is produced sometimes by a concentric arrangement of inclusions, some- 
 times by a variation of composition and extinction angles in different 
 layers. The zonal structure of the feldspars in these rocks is as per- 
 fect as it is in the more modern andesites. The mica in No. 11087 is 
 biotite of the usual character, but in No. 11089 muscovite is equally 
 abundant, making this latter rock a ^rue granite instead of a granitite. 
 Some of this muscovite, at least, may be plainly seen to have originated 
 from the alteration of the orthoclase. In many cases it lies in brilliantly 
 polarizing flakes of considerable size, clustered together in the center 
 of the orthoclase crystals, which portion always appears to be the most 
 subject to alteration. 
 
 These rocks show to a moderate degree the effects of pressure which 
 are most manifest in the porphyritic quartzes. These are much dis- 
 torted and often broken and granulated, as shown in PI. XV, fig. 2. 
 It seems at first thought strange that 
 the harder quartz should be more sus- 
 ceptible to pressure than the softer 
 feldspar, and yet this is known to be 
 a well established fact, as has been 
 observed in Chapter I. The brittle- 
 ness of the quartz causes it to break, 
 where the feldspar is only bent or 
 distorted, without rupture. 
 
 In some cases the feldspar, as well as 
 the quartz, 6hows a slight peripheral 
 granulation and passage into a mosaic, 
 which can not be distinguished from 
 the groundmass. This is in all in- 
 stances, however, only incipient, while 
 the main portion of the groundmass is an original feature of the rock. 
 
 In the granitites, Nos. 11087 and 11190 an unusual constituent is 
 present. This is in sharp crystals of good size (2 by 3""") and has the 
 shape of epidote. Its color is yellowish brown or greenish yellow. 
 
 Fig. 17. — Orthite in granite. Horae Race 
 Rapid. No. 11087. Magnified 80 diameters. 
 
118 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62 . 
 
 it seems to have undergone partial alteration, and agrees closely with 
 the published descriptions of orthite (allanite). 1 The two crystals in 
 section No. 11087, although by no means entirely changed, appear to 
 be completely isotropic, a peculiarity especially mentioned by Rosen- 
 busch as not uncommon to orthite. 2 
 
 Augen-Gneiss. — The best example of this type is No. 11184, from the 
 Michigan side of the Horse Race. With reference to this rock the fol- 
 lowing is extracted from the field notes made in July, 1885: 
 
 A short distance above the mouth of the Horse Race the ridge is cut by a ravine. 
 Here, near the water’s edge, are some beautifully porphyritic, red, acid rocks, occur- 
 ring apparently as dikes in the greenstone. The direction of these dikes is quite 
 irregular. Their width also varies continually. They contain a deep red feldspar, a 
 white feldspar, and quartz in porphyritic crystals. When much of the first mentioned 
 feldspar is present, the rock is very red ; when it is absent it is gray. Both varieties 
 may occur in the same specimen. These rocks show the effects of pressure very finely. i 
 The porphyritic crystals form “ Augen,” around which the groundmass bends. The 
 direction of the banding when well marked appears to be parall 1 to the walls of the 
 dikes. The “ Augen” stand vertically. 
 
 Under the microscope the banded or gneissic structure of this rock is 
 as well marked by the lenticular (“ Flaser ”) arrangement of the mica as in 
 the hand-specimen. Its most instructive feature is the formation of the 
 eyes (“Augen.”) and the gradual disappearance of the large porphy- 
 ritic feldspar crystals by peripheral granulation due to pressure. A ] 
 typical example of this is represented in PI. XV, fig. 1. Here it 
 will be seen that a large porphyritic crystal of triclinic feldspar has been 
 granulated on two opposite sides, corresponding to the direction of the 
 schistosity, and that the material thus formed has been drawn out into 
 a lenticular- shaped mass, with the remaining solid portion of the feld- 
 spar as its center. This forms the eye or “ Auge” around which the 
 groundmass is seen to curve. Such a structure has been described and 
 figured by J. Lehmann 3 and others. It is important to observe that the 
 secondary granulation has here produced a mosaic of much coarser grain 
 than the surrounding groundmass. This corresponds to observations 
 of Dr. Chelius, made on certain Hessian granite porphyries. 4 
 
 No. 11196, from the head of the Horse Race, on the Michigan side, is 5 
 
 described in the field notes as “ a typical biotite gneiss with a wavy I 
 
 structure, the biotite lamellae (secondary?) winding around the porphy- 
 ritic crystals of feldspar and quartz.” Under the microscope the ground- 
 mass is seen to be fine grained, and, to some extent at least, to have 
 originated from the granulation of the porphyritic crystals, which ex- 
 hibit this process in an admirable manner. Dark brown biotite and 
 sphene are common. Zircon and apatite are also present. The quartz 
 
 » 
 
 'A. Sjogren, Geol. Fiiren. Stockholm Forliandl., vol. 3, 1876, p. 258, Tbrnebohm Under Vega-Expe* j 
 ditionen insamlade hergarter. Vega-Exped. vetensk. jakttagelser, VI, Stockholm, 1884, p. 124. Cross 
 & Iddings, Am. Jonr. Sci., 3d series, vol. 30, 1885, p. 108. 
 
 2 Mikros. Pbysiog., 2d ed., vol. 1, p. 499. 
 
 3 Untersuclmngen iiber die Entstehung der altkrystallinischon Schicfergesteine. Eonn, 1884. 
 
 4 Notizblatt des Vereins fur Erdkunde zu Darmstadt, 4. Folge, 5 Heft., 1885, quoted by Roaenbusch, 
 Mikros. Pbysiog., 2d ed., vol. 2, p, 294. 
 
Williams.] SCHISTOSE PORPHYRIES OF THE a HORSE RACE.” 119 
 
 is in large granular areas. Rows of fluid cavities traverse the. grains 
 and pass uninterruptedly from one to another. 
 
 The following analysis of this rock is also by Mr. R. B. Riggs : 
 
 Silica (Si0 2 ) 67.77 
 
 Alumina (A1 2 0 3 ) 16.61 
 
 Ferric oxide (Fe 2 0 3 ) 2.06 
 
 Ferrous oxide (FeO) 1. 96 
 
 Lime (CaO) 1.87 
 
 Magnesia (MgO) 1.26 
 
 Soda.(Na,0) 4.35 
 
 Potash (K,0) 2.35 
 
 Water (H,0) 1. 69 
 
 Carbon dioxide (C0 2 ) 19 
 
 Total 100.11 
 
 This is much more like the analysis of a granitite than the last one 
 given (No. 11082), but the preponderance of soda over potash indicates 
 the presence of a large amount of soda orthoclase. 
 
 Schistose Porphyries or Porpliyroids. — Just below Upper Quinnesec 
 Falls, especially on the Wisconsin side, are good exposures of finely 
 schistose acid rocks. They contain small porphyritic crystals of feld- 
 spar and quartz, and a considerable amount of sericite or hydro-mica, 
 which winds around these crystals so as to produce a lenticular or 
 “ Flaser ” structure. In color they present every shade from flesh red 
 to gray. 
 
 Rocks of this general type have a wide distribution and have arrested 
 the particular attention of petrographical investigators. In some in- 
 stances they have been conclusively shown to be the product of the 
 metamorphism of fragmental rocks — either tuffs or true sediments — 
 while in other cases they have resulted from the action of great dynamic 
 forces upon massive rocks of a corresponding composition, i. e. quartz 
 porphyries. When it is possible to trace with certainty the origin of 
 these rocks to stratified deposits they are usually designated asporphy- 
 roids , while in case their mother-rock can be shown to have been quartz 
 porphyry they are usually called schistose porphyries. In their extreme 
 development these two types are often petrographically indistinguish- 
 able and they present an instructive instance of the production of identi- 
 cal results by the action of the same physical forces upon matter of the 
 same average composition, though differing widely in origin and its 
 structure. 1 
 
 The schistose porphyries occurring at Upper Quinnesec Falls were 
 made the subject of an extended paper by Hermann Oreduer, published 
 in 3870. 2 This author concludes from a macroscopical examination that 
 these rocks are altered sediments which are interpolated between the 
 
 ' Hull. U. S. Geol. Survey, No. 28, p. 1. 
 
 2 Uober Nordamerikani«cke Schioferporpliyroido. Nencs Jalirlmch fiir Mineral., 1870. pp. 970-984. 
 
120 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62. 
 
 diabase beds of tbe Upper Huronian. He divides their whole ex- 
 posure at this locality, which he gives as 300 feet, as follows: 
 
 Feet. 
 
 (b) Weakly schistose orthoclase porphyroid 50 
 
 (c) Typical feldspar-paragonite schist 10 
 
 (d) Light liesh-red orthoclase-paragonite schist 30 
 
 (e) Paragonite schist 15 
 
 (f) Lime-paragonite schist 15 
 
 (g) Light reddish gray schistose porphyroid 30 
 
 (h) Lime-chlorite schist 50 
 
 (i) Chlorite schist * 100 
 
 Total 300 
 
 Of (b), (c), (d), and (e) he gives the following analyses : 
 
 
 (b) 
 
 (c) 
 
 (d) 
 
 (e) 
 
 Si0 2 
 
 66. 70 
 
 72.45 
 
 76. 505 
 
 75.5 
 
 A1 2 0 2 
 
 15. 90 
 
 8.85 
 
 7. 950 
 
 8.6 
 
 Fe 2 0 3 
 
 4. 70 
 
 6. 20 
 
 8. 875 
 
 2.6 
 
 MnO 
 
 tr. 
 
 tr. 
 
 tr. 
 
 
 CaO 
 
 tr. 
 
 tr. 
 
 0. 322 
 
 7.2 
 
 MgO 
 
 
 
 tr. 
 
 1. 2 
 
 K 2 0 
 
 8. 06 
 
 9. 24 
 
 1.025 
 
 0.3 
 
 Na,0 
 
 5. 50 
 
 3. 70 
 
 4.384 
 
 3.0 
 
 H 2 0 
 
 
 
 
 1. 5 
 
 
 
 
 
 
 Total 
 
 100. 8G 
 
 100. 44 
 
 90. 061 
 
 99.9 
 
 In discussing these analyses Oredner finds sufficient proof that ortho- 
 clase alone is present, from the fact that the potash increases propor- 
 tionately with the amount of feldspar, and in the absence of a twinning 
 striation which is visible to the naked eye. The sodium he attributes 
 entirely to the mica, which, in consequence, he names paragonite. 
 The proof of sedimentary origin he finds in the constant parallelism of 
 the schist planes with the limit between these rocks and the adjoining 
 diabase ; and yet he cannot help being much struck with the alterna- 
 tion of such widely diverse rocks in a single and comparatively thin 
 complex. 1 
 
 My studies of these rocks, both in the field and in the laboratory, 
 have led me to results quite the reverse of those obtained by Credner. 
 Nos. 11050 to 11053 were collected from the most typical band, which 
 here stands nearly vertical and strikes 20° S. of E. They are all essen- 
 tially the same in everything except color. They contain more or less 
 rounded porphyritic crystals of quartz and a red or grayish feldspar, 
 imbedded in a matrix apparently composed of a yellowish gray, greasy- 
 feeling hydro-mica. >. 
 
 1 Dio ebenerwaknte Wecksellagerung vollkomtuen versckiedenartiger Gesteine ala zusammen" 
 gekdrige Glieder einer wenig niacktigen Sckicktenreilio ist lioekst aufiallig. Zwiacken zwei Lagern 
 von Diabas, also einom narqentlicli aus Kalkfeldspath und Augit bestekenden basiscken Gesteine rait 
 etwa 54 Proc. Kieaelsiiuro tritt zumickst eiuo Zone von sauren quarzreickon Kali fel d apafck-N at rongliru - 
 lncr-Porpkyroiden mit iiber 70 Proc. Kieselsaure, aber okuo Kalkgekalt auf,” etc. — Loc. cit., p. 981. 
 
williams.] SCHISTOSE PORPHYRIES OF THE “ HORSE RACE.” 121 
 
 The following analysis of No. 11050 by Mr. K. B. Biggs shows its 
 essential identity with Credner’s specimen (b). Almost the only dif- 
 ference is the smaller amount of alkali, although the relative propor- 
 tions remain about the same. Iu Credner’s analysis the CaO and 
 MgO, which make up this difference, do not appear to have been deter- 
 
 mined. 
 
 Silica (SiO,) 6G. 60 
 
 Alumina (A1 2 0 3 ) 16.69 
 
 Ferric oxide (Fe 2 0 3 ) 2. 06 
 
 Ferrous oxide (FeO) 93 
 
 Lime (CaO) 1.40 
 
 Magnesia (MgO) 1. 15 
 
 Soda (Na 2 0) 2.46 
 
 Potash (K 2 0) 5.23 
 
 Water (H 2 0) 1.70 
 
 Carbon dioxide (00 2 ) 1. 42 
 
 Total 99.73 
 
 This is evidently the analysis of an orthoclase rock, and yet the micro- 
 scope shows that a considerable proportion of the porphyritic feld- 
 spars are striated and triclinic, iu spite of the fact observed by Cred- 
 ner, that this character is not apparent to the unaided eye. We may 
 therefore reasonably suppose that the potash exists largely in the 
 grouudmass and in the secondary hydro-mica, which is to be regarded 
 as true sericite, and not paragonite as assumed by Credner. 
 
 The microscope discloses in all the thin sections of these rocks the 
 typical structure of a quartz porphyry modified, however, by the 
 action of great pressure. An idea of it may be obtained from PI. 
 XIV, fig. 1, which represents No. 11050. The fine grained, micro- 
 granitic grouudmass is still present, inclosing the porphyritic quartzes 
 and feldspars. The former often exhibit their characteristic dihexa- 
 hedral form, but they are broken and possess an undulatory extinction. 
 The feldspars are most instructive. They possess a sharply defined 
 crystal form which, however, has been cracked and the fragments have 
 been more or less separated in the direction of the schistosity, while 
 brightly polarizing sericite scales have been abundantly developed 
 in all the fissures. Sericite is also abundant in the grouudmass, where it 
 appears to have been formed from the orthoclase. Its scales are par- 
 allel throughout the rock, to which fact the schistose structure is al- 
 most wholly due. The original biotite of these rocks is now entirely 
 represented by a pale green chlorite. During the process of this al- 
 teration, iron has separated in the form of opaque, black grains; and, 
 in some instances (11050 and 11052), colorless but very highly re- 
 tractive grains have been produced. These sometimes possess a sharp 
 octahedral form and are probably anatase, formed from the titanic acid 
 of the original biotite, as described by Stelzner. 1 In and around this 
 chlorite, tourmaline is also abundant either in single individuals or in 
 groups of crystals. Zircon and apatite are sparingly present. One 
 
 1 Neuea Jalirbudi fur Mineral., 1884., vol. 1, p. 273. 
 
122 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 remarkably large (.4 x .04 mm ) crystal of the former mineral, which has 
 been curiously broken, is represented in Fig. 18, taken from No. 11052. 
 
 Calcite is not uncommon and is al- 
 ways of a secondary nature. In Nos. 
 11051 and 11053 it forms a more or 
 less complete border around the por- 
 phyritic crystals. 
 
 As already stated, all four speci- 
 mens collected from this locality are 
 essentially identical. No. 11053 is 
 more finely schistose, owing to its 
 more advanced stage of alteration 
 and the consequent greater produc- 
 tion of sericite. In spite of this, how- 
 ever, the. original structure is still 
 plainly visible. No. 11096 was ob- 
 tained on the Michigan side of the 
 river, at the foot of the Horse Race. It has a very pronounced schis- 
 tose structure, and, under the microscope, appears nearly identical 
 with the rocks just described from below the falls, but is not so highly 
 altered. Its biotite is in its original fresh state, its porphyritic crystals 
 are more intact, and sericite is not so abundantly developed. 
 
 Gneiss . — In addition to thenonporphyritic gneisses already described, 
 Nos. 11079, 11084, and 11085 (see pp. 114-115) one other may be men- 
 tioned, No. 11188, from the head of the Horse Race, on the Michigan side. 
 This is apparently a typical biotite gneiss, but it is seen to pass by 
 gradual transitions into the hornblende gneiss No. 11189 (see p. 108). 
 The microscope shows that there are many points of resemblance be- 
 tween these two rocks. In the present case, although quartz is abun- 
 dant, ampkibole and the same sphene observed in No. 11189 are frequent, 
 and the feldspar is of such a nature as to be sTibject to saussuritization. 
 
 Felsite . — True nonporphyritic felsite is not common among the acid 
 rocks of the area about the Upper Quinnesec Fall and the Horse Race. 
 The most typical specimen of this class is No. 11071, which occurs in 
 narrow bands in the schistose greenstones below the falls on the Mich- 
 igan side of the river. This is a very compact, flesh colored rock re- 
 sembling jasper. Under the microscope it is seen to be essentially 
 identical with the groundmass of the porphyritic rocks above described; 
 and even here stretched and distorted crystals of quartz and feldspar 
 are not entirely wanting, though they are rare. 
 
 There is, therefore, strong evidence in favor of the view that the acid 
 rocks of the Upper Quinnesec region are of eruptive origin ; that they 
 are to be regarded as apophyses w T hich diverged from the granitic mass, 
 to the south; and that their schistose structure, when present, is to be 
 attributed to secondary causes. 
 
 Fig. 18. — Broken zircon crystal in schistose 
 porphyry. Upper Quinnesec Falls. No. 11052. 
 Magnified 180 diameters. 
 
WILLIAMS.] 
 
 ERUPTIVE ORIGIN OF THE ACID ROCKS. 
 
 123 
 
 This evidence may be summarized as follows: 
 
 First. The structure of these rocks, as revealed by the microscope, 
 in spite of its frequently being disguised by the action of secondary 
 causes, is always that recognized as characteristic of massive or igneous 
 
 rocks. 
 
 Second. There are present in these gneissoid bands granitic facies 
 which agree exactly with the rock of the main granite area, and the 
 bands themselves are identical with others near the contact, which can 
 be plainly seen to be radiating apophyses or dikes. 
 
 Third. The schistosity of these bands is often independent of their 
 direction and agrees with the prevailing strike of the surrounding 
 greenstones. 
 
 Fourth. There is abundant microscopic evidence that the constitu- 
 ents have been fractured, stretched, and crushed since their solidill 
 ation. 
 
 The localities thus far considered on the Menominee Eiver, viz : 
 Sturgeon, Lower and Upper Quinnesec Falls, contain all the important 
 exposures of crystalline rocks, belonging to what Major Brooks has 
 regarded as the southern of the two belts of greenstone. If his loca- 
 tion of these rocks is correct, the members of the northern belt appear 
 upon the river at three points, viz: Four-foot Falls, Lower Twin, and 
 Upper Twin Falls, of which, however, the two latter are connected by 
 almost continuous rock exposures. These localities we shall now pro- 
 ceed to consider in detail. 
 
 FOUR-FOOT FALLS. 
 
 The exposures at this place are represented, together with those at 
 both the Twin Falls, upon Major Brooks’s map, which is here repro- 
 duced in PI. VI. The fall is hardly entitled to be so called, as the 
 rocks have formed nothing more than a rapid in the river. Just at 
 the foot of this rapid the river is crossed by the Chicago and North- 
 western Kailroad bridge, immediately beyond which a cutting has 
 disclosed some very instructive exposures of the greenstones. The 
 rocks may be seen in position on either side of the river for some dis- 
 tance above the bridge. Brooks distinguishes upon his map many 
 alternating beds of massive, schistose, and slaty rocks ( a to n in his 
 section). The beds here strike about S 80° E — nearly at right angles 
 to the direction of the river at this point— and yet are mostly schistose 
 on the Wisconsin side and massive on the Michigan side. This fact is 
 indicated on Major Brooks’s map and speaks strongly against the view 
 that the present foliation is due to original bedding. 
 
 The rock of the exposure which occurs farthest down the river 
 (Brooks’s a) outcrops somewhat less than a quarter of a mile below 
 the bridge. It was called by Wright a chloritic slate, 1 and by Wieh- 
 
 1 Geol. Wisconsin, vol. 3, j>. 712. 
 
124 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 maim a phyllite. Major Brooks himself designates it as a “light bluish 
 gray, shining clay slate , with strong cleavage and no distinguishable 
 bedding planes.” 1 It does not beloug to the rocks now especially under 
 consideration, but since it was studied carefully it may be described 
 here for comparison. This slate occurs in a bed, estimated by Brooks 
 to be 550 feet in thickness, on both sides of the river and in its bed. It 
 strikes nearly east and west and dips toward the north. In Brooks’s 
 collection this rock bore the number 2075 ; in the present collection it 
 is represented by No. 11152. 
 
 Under the microscope there are visible in the thin section of this 
 specimen unmistakable signs of sedimentary origin. Coarser and finer 
 areas alternate, the former being made up of clastic quartz grains, 
 either pure or mixed with iron hydroxide or chlorite, while the latter 
 are composed of an argillaceous substance, filled with extremely minute 
 muscovite or sericite scales and considerable carbonaceous matter. 
 Tourmaline needles are also occasionally seen ; and zircon too, either in 
 minute, whole crystals or as irregular fragments of larger ones, is not 
 infrequent. This rock belongs to the detrital iron-bearing series, the 
 boundary between which and the greenstone schists lies just above 
 this exposure. 
 
 The railroad which crosses the bridge at Four-foot Falls exposes this 
 same rock again in a cutting about a mile west of Iron Mountain. A 
 specimen from this locality, No. 11114, shows the same general charac- 
 ter as the last described rock, except that it is more crystalline. 
 Tourmaline is present as before, but anew crystallization of biotite has 
 largely replaced the chlorite. The carbonaceous material is less abun- 
 dant and what remains is in a much more finely divided state. The 
 clastic origin of the rock is still very apparent in the shape of its quartz 
 grains, which are here mingled with feldspar fragments, both plagio- 
 clase, microcline and orthoclase. 
 
 No. 11113, from a quartzite band intercalated in No. 11114, also con- 
 tains feldspar grains mingled with the quartz. Zircon fragments are 
 likewise present and a little biotite, which is no longer quite fresh. 
 This latter mineral shows in a beautiful manner the development of 
 secondary rutile needles, as in the kersantites. 2 
 
 Before speaking of the greenstones which occur along the river 
 farther north, it will be well to examine those exposed in the railroad 
 cutting at the western end of the bridge. These rocks are, for the 
 most part, massive, but they nevertheless display evidence of extensive 
 crushing and chemical alteration. No. 11178 represents the average 
 type. This is of a light green color, and in a hand-specimen quite 
 aphanitic. Both macroscopically and microscopically it resembles the 
 massive greenstones so abundant in and representative of the region 
 south of Marquette (see Pl.X, fig. 2). Miueralogically there is hardly 
 a trace of the original rock left. Almost colorless hornblende, pale 
 
 1 Geol. Wisconsin, vol. 3, p. 475. 
 
 2 Roseubusch : Mikros. Physiog., 2d od., vol. 2, p. 311. 
 
U. S. GEOLOGICAL survey 
 
 BULLETIN NO. 62 PL. VI 
 
THE LIBRARY 
 OF THE- 
 
 UHIYERSITY OF ILLINOIS 
 
Wlf.LIAMS.J 
 
 GREENSTONES NEAR THE FOUR-FOOT FALLS. 
 
 125 
 
 green chlorite, zoisite, leucoxene and a little calcite (all of secondary 
 origin) are the present constituents; and yet the original structure of 
 the rock is strikingly well preserved. When viewed with a com- 
 paratively low power, in ordinary light, the outlines of long, almost 
 acicular, feldspar crystals are very apparent, in spite of the fact that the 
 substance of the feldspar itself is changed to chlorite or zoisite. These 
 outlines of former crystals make a confused aggregate, but each indi- 
 vidual preserves its own proper form (idiomorphic in the sense of Ros- 
 enbusch). The angular spaces between the feldspars produce a typical 
 example of the ophitic or diabase structure, although no trace of a dia- 
 base mineral remains. 
 
 But the exposure is not throughout as massive as the specimen just 
 described. It is traversed here and there by schistose and wavy bands 
 which show indications of having been much crushed and rubbed. 
 Slickensides are abundant and lenticular fragments fit into one an- 
 other so as to, produce an imperfect sort of foliation. In other cases, 
 where the crushing has been more intense, the schistosity is more per- 
 fect. These bands all strike a few degrees north of west, being appar- 
 ently conformable to the slates below and the greenstone schists above. 
 This is a suggestivefact when it is remembered, as observed by Brooks, 
 that these slates owe their lamination to slaty cleavage (a product of 
 pressure), which seems to have obliterated the original stratification. 
 
 Ho. 11179, from one of the schistose bauds in the greenstone of this 
 cut, shows under the microscope the effects of great mechanical action. 
 Curving and interlacing areas of pale green chlorite and of a grayish 
 substance (perhaps the remains of titanic iron) form the main mass of 
 this rock. Thickly scattered through these are patches of a dark brown 
 substance, often showing concentric zones of a clear, transparent char- 
 acter. These look like opal, but their optical character shows them to 
 be single individuals of crystalline quartz. Imbedded in this material 
 of such pronounced secondary character, are fragments of feldspar, 
 which have been crushed or broken. These, as has been observed so 
 frequently before, are less changed chemically than those in the mass- 
 ive rock from which this schistose band has been derived. 
 
 Four specimens were selected to represent the series collected along 
 the river north of the railroad bridge. Two of these came from each 
 side of the river and illustrate both the massive and schistose bands. 
 
 Ho. 11176 was found on the Michigan (eastern) side, just above the 
 bridge. In color it is light green, and in structure it is massive. Under 
 the microscope it shows a pale hornblende in ragged and irregular indi- 
 viduals, feldspar, zoisite, chlorite, and leucoxene. Traces of an original 
 diabase structure are still abundant in this rock. The feldspars often 
 perfectly preserve their lath-like form and their twinning striation, while 
 the pale but compact hornblende occupies the intervening spaces, sup- 
 plying the place taken by the augite in fresh rocks of this type. 
 
 Ho. 11175, from the highest exposure on the Michigan side of Four- 
 
126 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 . 
 
 foot Falls, is quite schistose and of a much darker color than the last 
 rock. Under the microscope it is seen to possess a much finer grain 
 and to be composed of hornblende, chlorite, feldspar, quartz, and leu- 
 coxene. The hornblende is for the most part pale green, but that it 
 was bleached from the brown variety is shown by the numerous com- 
 pact brown cores which occur in the centers of the paler crystals. The 
 structure of this rock is purely granular, with no trace of the diabase 
 type which characterized the specimen last described. This fact and 
 the indication that the pale, fibrous hornblende was derived from a 
 compact, brown variety of the same mineral, render it probable that 
 this rock was originally a diorite, composed of feldspar and brown 
 hornblende, in which little or no pyroxene was ever present. The horn- 
 blende of this rock exhibits a structure quite similar to that described 
 by Becke 1 and Van Hise 2 as due to a secondary enlargement of the 
 crystals in a solid rock. 
 
 The accompanying figure represents the compact brown interior of a 
 hornblende individual, more or less sharply separated from a pale green 
 or colorless border of hornblende fibers, which possesses exactly the 
 same optical orientation as the core. 
 
 Evidence seems to be constantly ac- 
 cumulating that various minerals 
 may continue their growth by regular 
 accretions in solid rocks, whether mas- 
 sive or clastic. This fact is satisfac- 
 torily established at least for quartz, 
 feldspar 3 and hornblende. While not 
 in the least doubting the correctness 
 of the conclusions above cited in re- 
 gard to the secondary growth of horn- 
 blende, I must, however, confess that 
 the present isolated instance appears 
 to me hardly to offer conclusive proof 
 that the fibrous hornblende border is 
 a secondary crystalline enlargement. 
 Such an explanation is possible, but 
 the appearance can be equally well explained in my judgment, by as- 
 suming that the fibrous zone is the result of bleaching and fraying 
 out of originally compact hornblende crystals. This process would 
 naturally commence at the ends of the crystals and develop principally 
 in the direction of the cleavage, as is here seen to be the case. The only 
 difficulty with this explanation is the sharp line sometimes seen between 
 the brown and the fibrous hornblende. But such a sharp boundary is 
 rather the exception than the rule. 
 
 •Tscherrnak’s mineral, u. petrog. Mittbeil., vol. 5, 1883, pp. 158-59. (cf. Am. Jour. Sci., 3d series, vol. 
 33, p. 385, 1887.) 
 
 2 Am. Jour. Sci. 3d series, vol. 30. p. 231, Sept. 1885. A. Harker has also recently described similar 
 secondary enlargements of hornblende in a hornblendcpicrite from Anglesey. Geol. Mag., London, 
 3d series, vol. 4, 1887, p. 550. 
 
 3 See Irving and Van Hiso: Bull. U. S. Geol. Survey, No. 8. 
 
 Fig. 19. — Compact cores of hornblende sur- 
 rounded by a fibrous border, No. 11175, a schis- 
 tose greenstone from Four-foot Falls. Mag- 
 nified 180 diameters. 
 
WILLIAMS.] 
 
 GREENSTONES OF THE TWIN FALLS. 
 
 127 
 
 Nos. 11142 and 11143, taken from two contiguous bauds on the Wis- 
 consin side of the river, about midway between the two points which 
 furnished the last described specimens, represent Brooks’s localities l and 
 lc respectively. The first is schistose, the second massive. The first 
 is a pale and schistose aggregate of nearly colorless chlorite, light 
 green or colorless hornblende fibers, quartz and calcite. The second is a 
 much darker green mixture of feldspar, hornblende, chlorite and leu- 
 coxene. The first named of these components has frequently its crys- 
 tal form well preserved, which betrays the diabase character of the 
 mother rock. The leucoxene in this section, as well also as in Nos. 11175 
 and 11176, often possesses the spliene-like habit which has been figured 
 from No. 11189. (PI. XIII, fig. 1.) 
 
 THE TWIN FALLS. 
 
 About a mile above the last described rock exposure at the so-called 
 Four-foot Fall, the quiet course of the Menominee Fiver is again inter- 
 rupted by a very considerable outcrop of greenstone. This is almost con- 
 tinuous for half a mile, but at either end of it the river plunges over a 
 barrier of somewhat harder rock than usual and spreads out below it 
 into a small basin. The two little water-falls thus formed are known 
 as the Twin Falls. In Major Brooks’s report they are included in the 
 same map that shows the topography of the Four-foot Fall, 1 and that 
 portion of this map which gives the outline of the Twin Falls is 
 reproduced in twice the scale of the original on PI. VI. 
 
 All of these exposures belong to the northernmost of the two green- 
 stone belts of the Menominee Iron Basin. This is much more uniform 
 in its composition than the southern belt, in which the Sturgeon and 
 Quinnesec Falls exposures are located. Its rocks are altogether of a 
 dark green, almost aphanitic type, which, when they become schistose, 
 give rise to dark cliloritic slates. Neither the light colored, gabbro-like 
 greenstone, nor coarse diorites, like those of the Horse Face, nor bands 
 of acid rocks occur in the northern belt — at least, not at the localities 
 where this crosses the river. 
 
 The homogeneous character of the Twin Falls greenstones is largely 
 due to an advanced state of chemical alteration, which has obscured 
 its original grain. 
 
 The macrostruetural changes, whereby the compact, dark green rocks 
 are converted from a massive -to a schistose state, may be admirably 
 seen along the river banks at both the Upper and the Lower Twin 
 Falls. The foliation of the massive and already chemically altered 
 rock takes place in a somewhat different manner from that heretofore 
 described. There are none of the ragged u cross gashes ” and irregu- 
 lar, gaping seams (see Fig. 10, p. 81) which are so common at the expos- 
 ures along the southern belt. These seem to be the result of stretch- 
 ing in a solid or very nearly solid mass, but in the present case this 
 process is hardly apparent. 
 
 Geol. Wisconsin, vol. 3, p. 475, PI. IV. 
 
128 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 The first step toward the formation of a schistose structure in these 
 Twin Falls greenstones (and this is hardly ever absent) is the division 
 of the massive rock by two systems of joints, which stand about per- 
 pendicular to the surface and intersect at a varying but acute angle. 
 These joint systems divide the mass into diamond shaped or rhomboidal 
 prisms, the cross sections of which are well displayed upon the fre- 
 quent smoothly glaciated surfaces of the rock. The appearance of such 
 a surface is diagrammatically represented in Fig. 20. 
 
 Figs. 20-22 diagrams illustrating the transition from jointing to schistose structures in the green 
 
 stones at Twin Falls. 
 
 As we approach the schistose band in the massive rock these inter- 
 lacing rhombs become lengthened out more and more by an approxima- 
 tion to parallelism, between the two systems of joint-planes. (Fig. 21.1 
 
WlU.IAMS.l 
 
 FOLIATION PRODUCED BY SHEARING. 
 
 129 
 
 These elongated prisms finally become very much extended lenses, 
 which interlock and produce a well developed, wavy or even parallel 
 schistose structure (Fig. 22). The almost slaty rocks thus produced, 
 especially as seen at Lower Twin Falls, have a tendency to break, not 
 so much along a definite plane as parallel to a line — i. e., the direction, 
 normal to the surface, parallel to which the original joint planes ran. 
 It is difficult to obtain well shaped hand- specimens of these rocks, but 
 narrow rhombic prisms of almost any angle are easily procured. There 
 is an almost equal tendency to cleave along any plane which is parallel 
 to the longest axis of these prisms. 
 
 If the prisms due to the original joint planes were subjected to a lat- 
 eral pressure which developed in them a cleavage that successively ap- 
 proached more and more nearly to the long axis as the prism was length- 
 ened, this peculiar tendency to separate along a line rather than along 
 a plane is precisely the structure which we might suppose would result. 
 
 The strike of these schistose bands follows the direction which bisects 
 the acute angle of the rhombic prisms. This is for the most part from 
 S. 70° to 80° E., agreeing with the prevailing strike of all the rocks in 
 this system. There are, however, many exceptions, where these schistose 
 bands, even where near together, follow different directions ; for in- 
 stance, I observed, in the massive though jointed rock on the Michigan 
 side of Upper Twin Falls, two schistose chloride bands quite near 
 together, one having a strike N. 180° E., and the other S. 73° E., while 
 the dip of each was nearly vertical. Such cases are easily explicable on 
 the supposition that these bands were produced by mechanical agencies, 
 but it is quite impossible to reconcile them with the supposition that 
 these bands are in any way the result of sedimentation. 
 
 This type of schistose structure was also noticed to a slight extent 
 at some of the exposures of the lower greenstone belt — notably just 
 below Lower Quinnesec Falls on the Michigan (left) bank of the river 
 (see p. 84). It is, however, there the exception, and is peculiarly the 
 characteristic of the upper belt as exhibited at the Twin Falls. 
 
 LOWER TWIN FALLS. 
 
 The development of the foliation in the massive greeu stone is also 
 shown on a small scale, partic- 
 ularly on the left (Michigan) 
 side of Lower Twin Falls, 
 where there has been a slight 
 a mount of slipping along aline 
 of jointing. Fig. 23 gives a 
 diagrammatic idea of a speci- 
 men observed at this locality. 
 
 The area represented is about 
 three feet square. Through 
 the center runs a vein of white 
 quartz which has been depos- 
 Bull. 62 9 
 
130 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62. 
 
 ited by infiltration in tlie old joint seam. On the edges of this the rock 
 is perfectly schistose and chloritic, but it passes gradually, in the space 
 of a few inches, into the massive aphanitic greenstone, which composes 
 almost all of this exposure. Fig. 24 represents a polygonal block, 
 formed by the jointing of the massive greenstone, which has been 
 frayed out into a perfectly foliated chlorite schist by a slipping move- 
 ment against the adjoining blocks. 
 
 The extensive chemical alteration which has gone on in this green- 
 stone seems to render it peculiarly sub- 
 ject to such a fraying out into a chloritic 
 schist. This change takes place in cases 
 where a fresher and harder mass would 
 have received only a slickensides. 
 
 The Twin Falls greenstones are in- 
 teresting, in view of the macrostructural 
 alterations which they exhibit. Miner- 
 alogically they are all so much decom- 
 posed that they present but little which 
 is determinable under the microscope. 
 
 The least altered specimen collected 
 is No. 11140, from the east side of the 
 Lower Fall. Together with the speci- 
 mens shown in Figs. 23 and 24, it came 
 from a steep wall of massive and but little 
 jointed greenstone, which rises abruptly 
 from the water’s edge. Diamond jointed 
 and somewhat schistose rocks of the 
 same sort occur on the north (No. 11139) 
 and fissile chloritic slates (striking W. of 
 N. and dipping 70° to the north) to the 
 south of it. Under the microscope this 
 massive rock is found to be a confused 
 aggregate of pale green, somewhat fib- 
 rous hornblende, feldspar remnants, and 
 leucoxene, which possesses a sphene-like habit and rarely shows any 
 trace of its original ilmenite. The clearer areas, which represent the 
 former feldspar, are now so filled with actinolite, zoisite, and epidote 
 needles, that nothing regarding the former character of this mineral can 
 be learned. In this rock secondary biotite is also quite abundantly 
 developed, as was found so often to be the case in the Russian metamor- 
 phosed diorites described by Inostranzeff 1 . The original structure of 
 this rock is now disguised almost beyond recognition, but it seems to 
 have partaken more of the granular nature of a diorite than of the 
 ophitic nature of a diabase. 
 
 No. 11132, taken from the continuation of this mass on the opposite 
 J Studien iibermetam. Great., ©to., 1879, pp. 81, 82, 109-112. 
 
WILLIAMS. 1 
 
 ANATASE IN ALTERED DIABASE. 
 
 131 
 
 side of the river, is essentially identical with it, but in it the form of the 
 original feldspars is better preserved. These may. often be seen in 
 well formed, lath-shaped crystals, which, in spite of their extensive saus- 
 suritization, still retain distinct traces of their plagioclastic twinning 
 striae. This rock also, in distinction from the one last described, con- 
 tains some chlorite but no biotite. 
 
 These rocks, like so many others of the Menominee River greenstones, 
 are representative examples of the type called by Giimbel u Epidiorit,” 
 which is now generally conceded to be an altered form of diabase. 1 
 
 The rocks into which these least altered forms pass are representative 
 chlorite schists and slates ; and there can be no doubt that these latter 
 have also resulted from the extreme effects of those metamorphic agen- 
 cies which changed the eruptive diabase to the epidiorite. 
 
 No. 11130, collected just below No. 11132, and grading imperceptibly 
 into it, is a schistose rock, composed of bright green chlorite, finely 
 granular quartz and, perhaps, second- 
 ary albite. The leucoxene m this 
 rock is particularly interesting. It 
 still retains small ilmenite cores in 
 places, but it is broken and pulled 
 out in the direction of the schistosity. 
 
 A very considerable portion of this 
 leucoxene, especially around the edge 
 of the grains, is composed of highly 
 refractive and brightly polarizing, al- 
 though extremely minute, colorless 
 crystals. These have an octahedral 
 habit and resemble auatase (Fig. 25), 
 which, as both Diller 2 and Eosen- 
 busch 3 have shown, sometimes origi- 
 nates fiom the alteration of ilmenite 
 (cf. also Nos. 11050 and 11052 p. 121). 
 tities in this rock. 
 
 - At the northwestern corner of the basin, below the Lower Twin Fall 
 (see map PI. VI), the rock is rkomboidally parted and weathers to a 
 brownish color. In spite of its massive appearance it possesses a latent 
 tendency to cleave along the longest diagonal of the rhomboidal prisms, 
 and this tendency is intensified by weathering. Toward the east this 
 rock (No. 11128) passes gradually into corresponding slates (No. 11129). 
 Under the microscope these two rocks are seen to be in all respects the 
 equivalents of Nos. 11132 and 11130, above described. Their main dif- 
 ference consists in their being richer in iron, which has oxidized and 
 
 Fig. 25. — Auatase derived from ilmenite, No. 
 11130, from the Lower Twin Fall. Magnified 
 180 diameters. 
 
 Biotite also occurs in small quan- 
 
 1 Cf. Kosenbusoh : Mikros. Physio"., 2d ed., vol. 2, p. 205. 
 
 2 Neues Jahrbuch fur Mineral., 1883, vol. 1 , p. 191. 
 
 3 Mikros. Phyaiog., 1st ed., vol. 2, 1877, p. 336; 2d ed., vol. 1, 1885, p. 332, cf. also Schenck; Inaugural 
 Dissertation, Bonn., 1884, p. 25. 
 
132 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN 
 
 [BULL. 62. 
 
 stained the rocks brown. No. 11128 still retains much hornblende, feld- 
 spar, and ilmenite, and the diabase structure is still apparent in places. 
 No. 11129 is, like its counterpart No. 11130, a chlorite schist with the 
 hornblende replaced by chlorite, the feldspar by a quartz albite mosaic, 
 its leucoxene drawn out, and its structure wholly changed. 
 
 Perhaps the most altered rock of any encountered at the Lower Twin 
 Fall is No. 11139, which was one of the chloritic slates on the Michigan 
 side of the river below the massive rocks. This is a very fine grained 
 aggregate of pale green chlorite, quartz, or quartz albite mosaic and 
 biotite, the latter constituent being sparingly present. Sharply defined 
 crystals of tourmaline are also abundant in this rock. 
 
 UPPER TWIN FALLS. 
 
 At the Upper Twin Fall the same massive greenstones with a rhom- 
 boidal parting prevail, everywhere traversed by more or less schistose 
 bands. No. 11133 is the massive rock from the left or Michigan side 
 of the fall. It is much altered chemically, but preserves its original 
 structure almost perfectly. When examined by a low magnifying power 
 there is seen a network of light colored, lath shaped feldspar forms, 
 which are almost acicular, like those of a porphyrite. Between these 
 is an allotriomorphic mass of a dark gray substance, representing the 
 former augite, or possibly a glassy base. When examined more care- 
 fully with a higher power, the feldspar is found to be completely 
 replaced by a mixture of pale green chlorite and brown biotite in the 
 closest relationship, while in them an occasional crystal of zoisite is 
 imbedded. The darker interstitial mass is composed largely of fibrous 
 hornblende in shreds or confused, matted masses, but these are mingled 
 with much impure and indeterminable matter. 
 
 Two schistose bandshave already been mentioned on p. 129 as travers- 
 ing this rock in different directions. Of these, the one striking S. 73° E. 
 is the less schistose, and is represented by specimen No. 11135. Though 
 much more altered than the last, there are here also occasional unmis- 
 takable traces of the same ophitic structure. The representative of the 
 other band, No. 11134, is hardly more than a fine schistose aggregate 
 of chlorite, quartz, and calcite, with only the faintest indications of its 
 original structure, and yet here there are beautiful leucoxene borders 
 around unaltered cores of ilmenite. Narrow veins filled with a mixture 
 of calcite and chlorite traverse all these rocks. 
 
 On the opposite or Wisconsin side of the Upper Twin Falls the rocks 
 are apparently the same, but they show, nevertheless, important mi- 
 croscopic differences. The massive forms represented by Nos. 11122, 
 11125, and 11126, collected at different points between the falls and 
 the bridge, are fine and confused aggregates of pale green, fibrous horn- 
 blende, chlorite, zoisite, quartz, leucoxene, and occasionally (No. 11122) 
 a little biotite. All of these minerals are of secondary origin and in 
 
Williams.] 
 
 DIABASE TUFFS AT UPPER TWIN FALLS. 
 
 133 
 
 the process of their formation most of the traces of the former rock- 
 structure have been obliterated. Such traces as still remain indicate 
 that the mother-rock was a diabase, but there are seen none of the long, 
 acicular feldspar forms, discovered in the rocks from the opposite side 
 of the river. 
 
 The schistose bands interlaminated with these rocks are quite like 
 those already described. One of these, however, No. 11123, obtained 
 directly beside the falls, shows almost the only evidence of fragmental 
 origin anywhere observed in the Menominee greenstones. This con- 
 tains irregular and angular fragments of quartz and a slightly altered 
 feldspar of considerable size. These are imbedded in a matrix of irregu- 
 lar grain, composed of chlorite, calcite, quartz, and opaque iron oxide, 
 which is accompanied by leucoxene. The chlorite scales often have a 
 radially divergent arrangement around the larger included fragments 
 of quartz and feldspar. 
 
 Thin section, No. 11122, shows the contact of this schist with the mass- 
 ive rock. This contact is so sharp as to lend much additional proba- 
 bility to the idea that in this case the two rocks are of different origin. 
 
 Rocks of this kind are to be regarded as diabase-tuffs, similar to those 
 which are so largely developed around Marquette, and which are to be 
 described in the sequel. It is easy to see how essentially the same ma- 
 terial, whether produced as volcanic ash or as a massive rock, when 
 subjected for a long period to the action of the same metamorphosing 
 forces, would give rise to masses which, in certain cases, could not be 
 distinguished from one another. This is undoubtedly true of many 
 occurrences on the Menominee River, and hence we can speak with cer- 
 tainty only of those instances where sufficient of the original structure 
 is preserved to do away with all doubt. Between undoubted massive 
 rocks rendered schistose by pressure on the one hand, and fragmental 
 tuffs which have been more or less completely solidified by the same 
 agency on the other, there must therefore be rocks whose original form 
 must always be uncertain. 
 
CHAPTER IV. 
 
 
 — , 
 
 GREENSTONE BELTS OF THE MARQUETTE DISTRICT. 
 
 INTRODUCTORY. 
 
 a 
 
 Ever since tbe discovery of iron in the northern peninsula of Michi- 
 gan, in 1844, by Burt and Houghton, the region around Marquette has 
 received much attention from geologists. Although not eo early known 
 as the famous copper district of Keweenaw Point, this iron region has 
 divided the scientific interest which was before felt in the copper- 
 bearing rocks. 
 
 Douglass Houghton, 1 Locke, 2 Foster and Whitney, 3 Whittlesey, 4 
 
 Kimball, 5 Credner, 6 Brooks, 7 Wright, 8 Wadsworth, 9 Rominger, 10 and 
 Irving 11 have studied the general relations of the deposits, while micro- 
 scopical descriptions of some of the rocks have been given by Julien, 12 
 Wright, 13 Wichmann, 14 Pumpelly, 15 Wadsworth, 16 and Irving. 17 
 The city of Marquette is situated on the south shore of Lake Supe- 
 
 rior, about midway between the Carp River and the promontory kuown 
 as Presqu’ Isle, between which points (a distance of about 4 miles) the 
 lake shore runs nearly north and south. The city for the most part 
 lies within the square mile designated as Sec. 23, T. 48 K., R. 25 W., 
 Michigan. 
 
 An excellent idea of the topography of this region and of that ex- 
 tending for 18 miles back of it (i. e., westward from the lake) may be 
 obtained from the large colored map prepared by Dr. C. Rominger. 18 
 - — — . 1 
 
 I Brooks, Geol. Michigan, vol. 1, 1873, p. 13. 
 
 2 Geol. Michigan, vol. 2, 1873, p. 239. 
 
 3 Senate Docs., 1st session, 30th Congress, 1847— ’48, II, Doc. 2. Report on the Geology and Topog- 
 raphy of the Lake Superior Land Dist., Part II, Iron Region. 
 
 4 Proc. Am. Assoc. Adv. Sci., 1859, vol. xiii, part 2, pp. 301-308 ; ibid., 1875, vol. 24, part 2, pp. 60-72. 
 
 6 Am. J our. Sci., 2d series, vol, xxxix, 1865, pp. 290-303. 
 
 6 Zeitschr. Deutsch. geol. Gesell, vol. xxi, 1869, pp. 516-554. 
 
 7 Geol. Michigan, vol. 1, 1873, part 1. pp. 1-319. 
 
 8 “Geology of the Lake Superior Iron District’’ in Swineford’s History and Review of the Copper, 
 Iron, Silver, Slate, and other Material Interests of the South Shore of Lake Snperior, 1876, pp. 132-145. 
 
 9 Bull. Mus. Comp. Zool., Cambridge, vol. 7, No. 1. 
 
 10 Geol. Michigan, vol. 4, part x, Marquette Iron Region, 1881, pp. 1-154. 
 
 II Preliminary paper on an Investigation of the Archean Rocks of the Northwest ; Fifth Ann. Rep. 
 
 U. S. Geol. Survey, 1886, pp. 181-242. 
 
 12 Geol. Michigan, vol. 2, 1873, Appendix A. 
 
 13 Geol. Michigan, vol. 2, 1873, Appendix C. 
 
 14 “ Microscopical Observations of the Iron-bearing (Huronian) Rocks from the region south of Lake 
 Superior,” 1876, Geol. Wisconsin, vol. 3, pp. 600-656. 
 
 15 Am. Jour. Sci., 3d series, vol. x, 1875, pp. 17-21. 
 
 18 Bull. Mus. Comp. Zool., vol. 7, No. 1. 
 
 17 Bull. U. S. Geol. Survey No. 8, pp. 27-30. 
 
 18 Geol. Michigan, vol. 4, 1881, in pocket. 
 
 134 
 
WILLIAMS.] 
 
 THE MARQUETTE GREENSTONES. 
 
 135 
 
 The general trend of both the drainage and of the geological forma- 
 tions within this area is toward the east. The two main streams follow 
 somewhat irregular but approximately parallel (eastward) courses and 
 empty into the lake about four miles apart. The more northerly of 
 these is called the Dead River ; the more southerly the Carp. 
 
 The general surface of this area rises by degrees from the level of 
 the lake to an elevation of about 1,000 feet above the lake. This sur- 
 face is, however, extremely broken and hilly, being traversed by east 
 and west ridges composed of rows of rocky knobs. These elevations are 
 never over two hundred feet in height from the base ; usually they are 
 much lower (from one hundred to fifty feet or even less). They all have 
 rounded outlines produced by the wearing action of the great glacier, 
 evidences of which are everywhere apparent in the smoothly polished 
 and frequently striated rock surfaces. These knolls rise from the even 
 level of a plain produced by the glacial debris deposited between them. 
 
 An account of the general geological structure of the Marquette region 
 has already been given in Prof. Irving’s explanatory note at the begin- 
 ning of this paper, in which is included also a summary of the different 
 views held by various writers with regard to the stratigraphical posi- 
 tion and origin of the rocks of the greenstone-schist area, which forms 
 the subject of this part of the present essay. In connection with this 
 account has also been given a geological map of the Marquette region, 
 compiled by Professor Irving from the maps of Brooks and Rominger 
 and from original observations of his own. (PI. I.) It will not there- 
 fore be necessary for me to present anything further as to these general 
 matters in the present connection. 
 
 Special references to the petrographical work of others on the Mar- 
 quette rocks will be made in the course of the following detailed descrip- 
 tions. 
 
 In some respects the greenstones of the Marquette area seem pecu- 
 liarly suited to throw light upon the dynamic metamorphism of basic 
 eruptives, since a portion of these rocks seem to have been extruded 
 both during and subsequent to the action of the metamorphosing 
 forces. Hence we find the same eruptives in different stages of altera- 
 tion. Moreover, fragmental material (tuff) of the same nature and 
 origin of the massive rocks is abundantly developed, and this too 
 shows varying stages of consolidation into masses which closely re- 
 semble the solid rock. This great variety, while it is full of interest 
 and suggestions of new possibilities, is frequently very confusing. It 
 often becomes impossible to speak with certainty about the origin of a 
 rock which, on account of its many analogies, we may regard as hav- 
 ing been produced in several different ways. 
 
 The general similarity of the greenstone schists of the Marquette 
 and Menominee areas will be brought out in the following pages. It is 
 worthy of mention that the greenstone schists of both of these regions 
 have a strong resemblance to some of the greenstones and agglom- 
 
136 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62. 
 
 erates of the extensive group of rocks occurring on the Lake of the 
 Woods and on Bainy Lake in Canada, to which Mr. Andrew 0. Law- 
 son, of the Canadian Geological Survey, has given the name of Kee* 
 watin series. This series he regards as belonging immediately be- 
 neath the Huronian, which is represented in those northern regions 
 by the so-called Animike series. 1 This is also the position which the 
 greenstone schists of Marquette occupy, since they quite unmistak- 
 ably underlie the iron-bearing detrital rocks, which, according to 
 Irving, are the equivalents of the true Huronian. According to Irving 
 also the greenstone schists here probably underlie the overlying iron- 
 bearing series unconformably. 
 
 The Marquette greenstone-schist belt, which at the lake shore is 
 between 2 and 3 miles wide, extends to the westward for about 6 miles, 
 without materially altering its form or width. It then broadens sud- 
 denly by a wide extension toward the north, and at the same time is 
 divided into two portions by the eastern extension of a narrow arm of 
 granite (See map, PI. I). The southern of these portions continues a 
 due westward course with an average width equal to that of the entire 
 belt before its division. The northern portion is separated from the 
 southern, first by granite, and then to a greater and greater extent by 
 a large, wedge shaped area of the rocks of the overlying iron-bearing 
 or Huronian series. 
 
 For convenience in arranging the following petrographical descrip- 
 tions the ground covered has been divided into four areas, which will 
 be considered in order: (1) The eastern area, near Marquette; (2) the 
 western area, immediately north of Teal Lake, in the town of Negaunee ; 
 (3) the northern area, lying north of Dead Biver, and (4) the Deer Lake 
 area, a short distance north of the town of Ishpeming. The last named 
 area was not studied by the writer in person, specimens from it, with 
 full descriptive notes, having been sent to him by Professor Irving for 
 comparison with the collections which the writer had himself made in 
 other areas. 
 
 In the eastern or Marquette area the whole width of the greenstone 
 belt, including the granite contact on the north, was studied for a 
 distance of 3 miles west from the lake shore. In the western or 
 Negaunee area two sections were run northward across the greenstone- 
 schist belt, one passing through Secs. 21, 28, and 33, T. 48 N., B. 26 
 W. ; the other through Secs. 13, 24, 25, and 36, T. 48 N., B. 27 W. 
 In the northern area the examinations made were carried on from a 
 camp situated in Sec. 9, T. 48 N., B. 26 W., and embraced the area 
 covered by Secs. 3, 4, 5, 8, 9, 10, and 11 of this township. 
 
 The first of these areas is the most varied in its petrographical 
 characters, and it was, therefore, the most thoroughly studied. It is 
 
 *See General Report of Progress of the Geological Survey of Canada for 1885; also of Am. Jour. 
 Sci. (3d series), vol. 33, 1887, p. 473. I am indebted to Dr. Lawson for the opportunity of examining 
 the extensive suite of the Rainy Lake rocks, upon the microscopical study of which he was engaged 
 in the petrographical laboratory of Johns Hopkins University in the winter of 1886-’87. 
 
WILLIAMS.] 
 
 DIVISIONS OF THE MARQUETTE AREA. 
 
 137 
 
 divided into two portions of nearly equal extent by the narrow east 
 and west band of iron-bearing slates, to which Rominger applied the 
 name of Eureka series. The northern portion of the Marquette area, 
 extending from Lake street, Marquette, northward to the granite, is in 
 large part composed of banded greenstone schists, having an east and 
 west strike, and a steep northern dip. They are most conveniently seen 
 in typical development on Lighthouse Point. The layers of these rocks 
 are alternately of a darker and lighter shade of green, which gives these 
 particular greenstones their characteristic striped appearance. In these 
 banded rocks of the northern part of the Marquette area intrusions of 
 comparatively little altered acid and basic matter are abundant. These 
 are for the most part conformable to the bedding of the schists and 
 embrace granites, gneisses, schistose porphyries, diorites, and diabases. 
 Whenever, in these undoubtedly eruptive rocks, a schistose structure 
 is apparent, this is conformable to the bedding of the banded green- 
 stone schists. 
 
 The southern portion of the area about Marquette, on the other 
 hand, is occupied by much more massive and homogeneous greenstones 
 of a nearly uniform light green color, and an almost aphanitic struct- 
 ure. These are characterized by their division into oval or lenticular 
 areas which interlace and which are separated by a finely schistose 
 material of much finer grain. This peculiar parting, which, accord- 
 ing to the writings of the Canadian geologists, appears to have a very 
 widespread distribution through the greenstones of the Northwest, at 
 first glance resembles the spheroidal weathering of many eruptive rocks. 
 There is, however, better reason for regarding it as of mechanical 
 origin, as will be more fully explained in Chap. V. 
 
 The schistose structure of the southern Marquette greenstones is of 
 secondary origin, due, probably, in almost every case, to pressure, while 
 anything like the banding or striping of the more northern rocks is here 
 wholly wanting. Intrusive rocks are rarer than in the banded green- 
 stones of the northern portion of this area. When such dikes do occur 
 they are much more altered and hence approach closely to the enclos- 
 ing rock — a fact which renders their detection difficult. 
 
 The two portions of the Marquette greenstone area are therefore 
 broadly distinguished in many of their petrographical characters. The 
 east and west band of iron shales, mentioned above as separating 
 them, extends from the north side of Marquette harbor (Lake street) 
 westward along the northern side of the Duluth, South Shore and 
 Atlantic Railroad. They seem to be identical with certain members of 
 the iron series and at one point, about two miles west of Marquette, they 
 actually contain quite an extensive deposit of hematite. It is here 
 that the Eureka shaft was sunk at an early date in the history of iron 
 mining in the Marquette region, and from this Dr. Rominger has taken 
 his name for this series of Huronian beds. To make the references to 
 localities in the Marquette area more intelligible, a sketch map of the 
 environs of the city is here appended, PI. VII. 
 
138 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62. 
 
 With reference to the other two areas examined it is here sufficient 
 to say that the greenstones of the western or Negaunee area more 
 closely resemble those exposed in the southern portion of the Marquette 
 region ; while the rocks encountered in the northern area show many 
 points of likeness to those occurring north of Marquette. 
 
 ROCKS OF THE NORTHERN PORTION OF THE MARQUETTE AREA. 
 
 BASIC INTRUSIVES. 
 
 Diabase . — Diabase in well defined dikes of various sizes is an impor- 
 tant feature in the geology of the northern portion of the Marquette 
 greenstone area. This rock occurs in all stages of preservation from 
 an unaltered condition to a hardly recognizable aggregate of secondary 
 and decomposition products. 
 
 In all the freshest specimens examined olivine is present, but with 
 the commencement of alteration this mineral is the first to disappear 
 In many cases, therefore, where the rock may still be recognized as a 
 typical diabase, it is now impossible to say whether it was originally 
 olivine-bearing or not. 
 
 The next stage in the alteration is marked by the change of the 
 pyroxene to uralite, and the more or less synchronous passage of the 
 feldspar into saussurite and of ilmenite into leucoxene. 
 
 Still later follows the development of such final decomposition prod- 
 ucts as chlorite, epidote, calcite, quartz, etc. The extent to which these 
 chemical changes destroy the original diabase structure differs in dif- 
 ferent cases. As a rule this remains distinct during the first two stages 
 of alteration, while it generally, though not always, disappears during 
 the third. In some instances a pronounced schistose structure has 
 been developed in undoubted diabase dikes by extensile alteration. 
 
 The Great Dike . — The best material for the study of the fresh olivine 
 diabase near Marquette was obtained from the great dike which forms 
 the center of Lighthouse Point (see Pis. I and VII). Here its eruptive 
 character may be admirably seen by the sharp line of contact which it 
 presents with the adjoining banded green schists. This dike may be 
 traced by several outcrops along Michigan street in Marquette, and 
 then as a high, rocky ridge which extends for some three miles westward, 
 through Sections 15 and 16, just north of the main road from Marquette 
 to Negaunee. 
 
 From various portions of this dike nine specimens were collected. 
 The four freshest of these specimens (Nos. 11617 and 11622, from Light- 
 house Point ; No. 11636, from Lighthouse Point quarry, and No. 11666, 
 from a cutting on Michigan street) are not to be distinguished from 
 one another. 
 
 The structure of this work is the hyp-idiomorphic diabase struct- 
 ure, 1 which forms one of the most certain characteristics of this group 
 
 ^‘Structure ophitique” of Fouqu6 and Miehel-Levy, “ Divergent-strahligkornige Strnctnr ” of 
 Lossen, and “ Diabasischkdrnigo Structur ” of Roaenbuscli. 
 
U. S. GEOLOGICAL SURVEY 
 
 BULLETIN NO. 62 PL. VII 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
 
wiuiAMs.) DIABASE OF LIGHTHOlfSE POINT DIKE. 139 
 
 of eruptives. The grain is of medium coarseness. The lath-shaped 
 plagioclase crystals measure from 1.5 to l mm by 0.25 to 0.15 mm . The 
 interstices between these are filled with augite and ilmenite. The min- 
 eral components observed under the microscope are, in order of their 
 age, as follows : 
 
 Essential ; Olivine, labradorite, augite, \ Magnetite. \ 
 
 Accessory : Apatite, hornblende, biotite, quartz. 
 
 Secondary : Serpentine, uralite. 
 
 The olivine is mostly in rounded grains or in irregular areas, although 
 it sometimes shows evidences of a crystal form, especially the acute 
 angle due to the intersection of two dome faces (notably in No. 11666). 
 It is commonly wholly changed to serpentine, but in a few instances 
 remnants of the original transparent olivine substance remain. 
 
 The feldspar is always a plagioclase with the peculiar elongation of 
 the crystal in the direction of the brachydiagonal axis, which is charac- 
 teristic of diabase. The crystals are always striated, often minutely so. 
 The extinction is generally sharp, although an undulatory extinction 
 is sometimes observed. 
 
 The augite is quite normal for diabase. It is of a light, slightly 
 reddish shade of gray, with a perfect cleavage parallel to the prism. 
 Twins are very common, and the line of the lamellae may be seen in 
 ordinary light traversing the basal sections and bisecting the cleavage 
 angles. In polarized light the colors distinguishing the twin lamella? 
 are very brilliant. No crystal form is ever recognizable, the mineral 
 being typically “ xenomorphic,” in the sense used by Kohrbach. 1 
 
 Quartz is rare in diabase, but where it occurs as it does in No. 11666 
 we must regard it as an original constituent, on account of the extreme 
 freshness of the whole specimen. 2 
 
 The iron oxide is entirely opaque and shows a very irregular outline. 
 This is mostly due to the penetration into it of the feldspar crystals 
 whose form is clearly shown. Its crystallization must therefore have 
 been subsequent to that of the feldspar, and was apparently about 
 synchronous with that of the augite. The oxide itself is probably 
 partly ilmenite and partly a titaniferous magnetite. In none of the 
 freshest specimens does it show trace of leucoxene. It is, however, 
 sometimes partially surrounded by a border of biotite. 
 
 Original hornblende is rare in this rock, but traces of it were 
 observed in a few instances. 
 
 Among the alteration products serpentine is abundant wherever 
 olivine existed, but the rock is still too fresh to show more than the 
 most occasional uralitization of the pyroxene. 
 
 The five other specimens collected from this great dike show more 
 
 1 Tsehermak’s mineral, u. petrog. Mittheil., vol 7, 1885. Rolirbacli’s two terms, “authomorphic’* 
 and “xonomorphic,” adopted by Kalkowsky (Litbologie, 1886, p. 14) wore replaced by Rosonbusch in 
 the last edition of his Massige Gesteine by “ idiomorphio ” and “ allotriomorphic.” though for what 
 reason is not apparent. 
 
 2 Cf. Rosenbasch, Mikros. Physiog., 2d ed., vol. 2, 1886, p. 188. 
 
140 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 . 
 
 altered forms or abnormal varieties of the same rock. They are as 
 follows : 
 
 No. 11621, glassy diabase. 
 
 No. 11675, granophyre diabase. 
 
 No. 11672, uralite diabase (structure intact). 
 
 No. 11615, uralite diabase (structure intact). 
 
 No. 11610, epidiorite schist (structure gone). 
 
 No. 11621, collected near No. 11622 from the side of the great dike on 
 Lighthouse Point, is a glassy modification of the diabase, produced by 
 the rapid cooling of the molten mass against the inclosing walls. The 
 microscope shows this rock to be composed of a very dark brown glass, 
 which can be rendered transparent only with the greatest difficulty. 
 This opacity is due to the accumulation of minute globulitic bodies, 
 which can be detected only with the highest magnifying power in the 
 thinnest parts of the slide. Traces of the arborescent and fern-like forms 
 common in basic glasses (tachylite) are easily recognizable. The only 
 mineral constituents which have crystallized in this rock are olivine 
 and feldspar. The former shows well defined crystals. These fre- 
 quently contain inclusions of the brown glass, and are now wholly 
 changed to a yellowish green serpentine. The feldspar shows the nar- 
 row, lath-shaped, and but partially completed crystalloids and skeleton 
 forms which abound in all glassy rocks. These are filled with either 
 penetrations or inclusions of the brown, glassy base. 
 
 The chemical constituents of the other diabase minerals — augite, 
 ilmenite, etc., are still present in the glass. 
 
 No. 1167 5 presents an unusual modification of this diabase. The speci- 
 men was collected from the high, rocky ridge which is formed by the 
 great dike in the southern part of Section 16, about one and a half 
 miles west of Marquette. The hand-specimen is browner than is usual 
 in this diabase and is speckled with reddish spots. Under the micro- 
 scope the grain is found to be of the usual coarseness and the rock 
 itself slightly more altered than the specimens above described. 
 
 The structure of the rock is still perfectly preserved. The ilmenite 
 is unaltered, and, as before, is frequently fringed with biotite. The feld- 
 spar is clear and its twinning striations are very distinct, although it is 
 traversed by many interlacing veins of a green chloritic alteration pro- 
 duct. There are no certain traces of olivine in this rock and the augite 
 has undergone extensive change to a brownish yellow hornblende. 
 This is partly fibrous, but also in part quite compact. Indeed, this rock 
 offers a noteworthy instance of the apparent change of augite directly 
 into compact brown hornblende. Much more of this mineral is here 
 present than in any of the fresher specimens examined. It is impossible 
 to assert positively that some of it did not exist as an original com- 
 ponent of the rock, but the frequent cases of its undoubted derivation 
 by paramorphism of the augite makes it at least probable that all the 
 hornblende has originated in this way. 
 
 The reddish spots spoken of as visible in the hand-specimen represent 
 another interesting feature of t hi ^ r.ick. They are shown by the micro* 
 
williams.] ALTERED DIABASE OF THE GREAT DIKE. 141 
 
 scope to be areas of a regular intergrowth of feldspar substance and 
 quartz. This is sometimes in the form of granophyre. i. e., in slender 
 fibers, which group themselves in radiating tufts about a clear feldspar 
 crystal, and sometimes it shows the structure called micropegmatite. 
 This latter consists of small angular areas of quartz, each having the 
 same optical orientation, which are embedded in the reddish globulitic 
 feldspar substance. 1 
 
 Quite recently Mr. Waldemar Lindgren has described a similar struct- 
 ure in a diabase from the Big Belt Mountains, Montana. 2 
 
 It was also observed by the writer some years ago in a diabase from 
 Pleasant Valley, New Jersey, a specimen of which he received from 
 Mr. J. F. Kemp, of Cornell University. 
 
 Rosenbusch 3 regards this structure as sufficient proof that the quartz 
 is original, but the observations of Irving 4 in the Keweenawan felsites 
 and others make this conclusion doubtful. 
 
 No. 11672, collected at the corner where the road running west from 
 Collins Furnace joins the road leading to Bancroft on the Dead River 
 (center of Sec. 17, T. 48 N., R. 25 W.), is a uralite diabase, whose 
 structure is still perfectly preserved. 
 
 The large crystals of idiomorphic feldspar are in part clear, but to 
 a considerable extent clouded by the development of saussurite. 
 
 The allotriomorphic augite is in some cases intact or remains as a 
 core in the center of the secondary hornblende which has been derived 
 from it. More frequently, however, the hornblende or uralite has wholly 
 replaced the pyroxene. Its structure is oftener compact than fibrous, 
 and its form reproduces exactly that of the original augite. Quartz 
 areas are not uncommon. The ilmenire is mostly changed to leucoxene. 
 Near one large grain of the latter is seen an area of brown mica, which 
 is filled with a sagenitic network of minute rutile needles. 
 
 No. 11615, from an outcrop of this same great dike, at the bottom of 
 the hill, which forms the eastern end of Arch street, Marquette, repre- 
 sents the next stage of alteration in the diabase. 
 
 The original structure is still plainly recognizable, although it is be- 
 ginning to be concealed by alteration. 
 
 The feldspars exhibit their characteristic lath-like forms, but the 
 sharpness of the outlines and more or less of the internal substance is 
 clouded by secondary products. These seem to be for the most part 
 small hornblende needles which have wandered in from the alteration 
 of the pyroxene, but in some places epidote is also developed from the 
 alteration of the feldspar itself. Still, in nearly every case enough of 
 this unchanged feldspar is present to show plainly its original form and 
 twinning structure. 
 
 'This peculiar structure was first observed in diabase by Tornebolim in 1877 (Neues Jahrbuch 
 fiir Mineral., 1887. p. 262), who found it in his Konga-diabase type of southern Sweden, and named 
 it “ Schriftfeldspath.” 
 
 2 Tenth Census Repta., U. S M vol. 15, 1887, p. 736. 
 
 * Mikros. Physiog. 2d ed., vol. 2. 
 
 * Cf. Mon., U. S. Geol. Survey vol. 5, p. 114. 
 
142 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 . 
 
 The augite is in the process of changing to hornblende. This altera- 
 tion is sometimes complete, but oftener cores remain in the center of 
 what was the original pyroxene crystal. The border of hornblende is 
 double, consisting of a wider internal band of yellowish brown fibers 
 which have apparently resulted directly from the augite substance, and 
 a narrower, outer zone of bright emerald green, pleochroic needles 
 which seem to project into the surrounding feldspar. 1 The individuals 
 of the inner zones are much smaller than those of the outer, and form 
 a confused, felt-like mass, while the external needles as a rule have 
 their longest axes parallel. These needles are most developed in the 
 direction of the vertical axis of the augite. They may owe their differ- 
 ent coloring to the influence of the feldspar substance which has con- 
 tributed to their formation. In some cases the secondary hornblende 
 appears to be homogeneous over considerable areas, exhibiting a uni- 
 form extinction and a comparatively compact character. This can not, 
 however, be regarded as original in its nature. 
 
 The ilmenite still retains its form but is largely changed to leucoxene. 
 
 No traces of olivine were found in this rock, probably because of its 
 altered condition. 
 
 No. 11616 is instructive when taken in connection with the specimen 
 last described, No. 11615. Both were collected from the large and 
 smoothly glaciated surface of trap, exposed at the east foot of Arch 
 street. Through the massive rock run a number of schistose bands, 
 produced by crushing and shearing along lines of weakness. One of 
 these bands furnished the present specimen. There can be no doubt 
 that these bands are a part of the massive rock. Both were the same 
 before the schistose bauds were produced by more intense mechanical 
 and chemical action. 
 
 Under the miscroscope the appearance of these two specimens is 
 found to accord fully with their field relations. Thb original diabase 
 structure, so distinct in the massive rock, has wholly disappeared in the 
 schistose one. There are no traces of lath-shaped feldspar left. The rock 
 is mainly composed of a confused network of fibrous, very pale green 
 and slightly pleochroic hornblende needles. These are sufficiently par- 
 allel in their arrangement to produce the schistose structure of this 
 rock. They are secondary — formed from the alteration of the augite or 
 the joint alteration of the pyroxene and feldspar — as maybe admirably 
 seen in section No. 11615, where they are in the process of formation. 
 Scattered among this hornblende, is considerable cloudy and nearly 
 opaque saussuritic substance, mixed with more or less secondary quartz, 
 both of which have been derived from the feldspar. The ilmenite also 
 has undergone an interesting alteration and is here represented by 
 cloudy leucoxene, with only occasional opaque black dots of the origi- 
 nal mineral. This substance is arranged in long stringers and shreds 
 which follow the direction of the schistose structure. 
 
 'On the production of a similar double uralit© zone around pyroxene. See Lessen : Erliiut. z. geol. 
 Specialkarte von Preuaaen u. d. tliiiring. Staaten, Blatt Harzgerode, p. 81, 1882 ; and Williams; Bull 
 U. S, Geol. Survey, No. 28, p. 42, PI. I, Fig. 2. 
 
WILLIAMS.] 
 
 THE BROOK SECTION. 
 
 143 
 
 Here we have an undoubted instance of the dynamic metamorphism 
 of a diabase, where every stage in the process can be followed. Every 
 mineral of the schist can with certainty be traced to its original form, 
 and yet the chemical alteration has been accompanied by such a change 
 of position (migration) that the original structure has wholly disappeared 
 and a new and different structure has been produced. This derived 
 rock is quite identical with some of the most characteristic so-called 
 hornblende or actinolite schists. 
 
 The chemical action has here been proportionately increased by the 
 crushing. This seems true for all the constituents, as there are no 
 traces of the fresh fragments of broken feldspar crystals which were so 
 often observed in analogous greenstones of the Menominee region. 
 
 There is an excellent section through the rocks of the northern por- 
 tion of the Marquette area, exposed by a brook which flows northward 
 almost along the line between Sections 15 and 16 (hardly over a mile 
 west of the city) and empties into Dead River. Between the road lead- 
 ing from Marquette to Collins’s Furnace and that forming the main high- 
 way toNegaunee, this small stream has excavated a deep ravine, upon 
 the high, steep sides of which the relationship of the different rocks is 
 admirably diplay ed. This locality is described by Dr. Rominger, 1 and 
 for convenience we will in future allude to it as the Brook section. 
 (See PI. VII.) 
 
 Here were encountered several exposures of fresh olivine diabase. 
 One of these, No. 11708, was taken from the branching dike in the 
 wall of greenschist and granite, which Rominger has described and 
 figured. 2 This rock resembles the freshest specimens obtained from 
 the great dike, except that its grain is finer, as might be expected in 
 a mass of so much smaller size. No trace of alteration is here visi- 
 ble, except in the olivine. This constituent is not abundant, but it 
 occasionally appears in well shaped crystals, which are completely 
 changed to yellow serpentine. The iron oxide presents in its form a 
 decided contrast to that above described. In this rock it was produced 
 much earlier than in the other, and hence it has a well developed crystal 
 form. This, as seen under the microscope, is square (octahedral section), 
 which may be an indication that the mineral is magnetite instead of 
 ilmenite, as before. The feldspar and pyroxene of this rock need no 
 special comment. 
 
 No. 11719, obtained near the edge of another dike not far from the 
 last mentioned one, is only semi-crystalline. Its brown, glassy base re- 
 sembles that of No. 11621, but crystallization is farther advanced. The 
 sharply defined olivine and feldspar crystals are quite the same, but a 
 vast number of smaller feldspar crystals are here developed in the base. 
 Only a very little augitc, and that in rounded grains, is present. This 
 rock would be correctly termed a raelaphyre. 
 
 •Geol. Michigan, vol. 4. p. 25, 
 ‘Ibid., p. 148. 
 
144 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62 . 
 
 No 11679 is from the center and No. 11680 from the edge of a dike 
 of porphyritic greenstone, which intersects the banded green schists on 
 the western side of the Brook section, not far from its southern end. 
 
 The first of these rocks has a coarsely porphyritic structure, which, 
 on account of its altered condition, is only prominent on a weathered 
 surface. A fresh fracture appears of an almost even gray color, re- 
 sembling some of the finer greenstones. Under the microscope this 
 specimen is found to correspond admirably to the descriptions of 
 the rock-type, named by Giimbel “ epidiorite.” The augite, reddish 
 brown cores of which still remain, is largely changed to fibrous horn- 
 blende. This mineral is mostly of a pale brown color, but often has a 
 bright green edging where it adjoins the feldspar substance, as has 
 already been noted in the case of No. 11615 (p. 141). The feldspar is 
 still clear and fresh, showing the characteristic lath-shaped forms of 
 diabase. It is only rarely clouded by small patches of a gray saussurite. 
 Much more abundant in this feldspar are veins and small areas of green 
 hornblende needles, which owe their existence mostly to the pyroxene, 
 though the feldspar seems also to have aided in their formation. They 
 are especially abundant in cracks, along which the substance appears 
 to have wandered from the decomposing augite. This hornblende is 
 finely fibrous and forms matted, felt- like masses. There is but little 
 chlorite and secondary quartz in this rock. The ilmenite is largely 
 changed to leucoxene and occasionally surrounded by a rim of biotite. 
 
 The second of these two specimens (No. 11680) from the edge of this 
 dike, shows an extremely fine grained, greenish groundmass, whose 
 components are very weakly polarizing and hardly determinable. This 
 was perhaps once a glass which has become devitrified and viriditic. 
 In it are imbedded sharp, lath-shaped plagioclase crystals, which are 
 either unaltered or at most penetrated by veins of actinolite needles, 
 and augite almost wholly changed to hornblende or chlorite. 
 
 The following five rocks are also good representatives of the epidio- 
 ritic type. They are largely composed of either light or dark green, 
 fibrous, secondary hornblende. In none of them does any trace of au- 
 gite now remain, and it is possible that some of them were originally 
 true diorites, like the rocks to be described under the next head. How- 
 ever, the unmistakable evidences of diabase structure often apparent 
 render it more probable that these rocks all belonged originally to this 
 type. 
 
 No. 11663, from Pine street just north of Michigan street, Marquette, 
 is most like a true diorite and may be an altered form of the Picnic Isl- 
 and rock. The hornblende is of the general type represented in PI. XII, 
 fig. 2 of No. 11186, from the Horse Race above Upper Quinnesec Falls 
 (see p. 107). It is more or less fibrous, of a pale green color and often 
 looks as though it had originated from the bleaching and disintegration 
 of a compact original hornblende. Around the edge of large areas it 
 has a darker green border and seems to ravel out into fine fibers which 
 
WILLIAMS. ] 
 
 EPIDIORITES. 
 
 145 
 
 wander into the feldspar. Indeed, the feldspar is quite filled with such 
 hornblende needles, which, together with its saussuritic alteration prod- 
 ucts, almost conceal the original substance. Ilmenite in ragged areas, 
 but without leucoxene, and a little of the chlorite-epidote aggregate (see 
 PI. XI, fig. 1) are also present. 
 
 Nos. 11712 and 11720, both from the Brook section, are rocks of the 
 same general character as that last described. The former is decidedly 
 schistose and bears much internal evidence of the action of great press- 
 ure. All of the constituents are arranged in interlacing and elongated 
 bands. The feldspar is much crushed and shows the peculiar mosaic 
 due to secondary crystallization. It is also often changed to a granular 
 aggregate of brightly polarizing, pale green epidote grains. The horn- 
 blende crystals are broken and bent, and especially around their outer 
 edge, are very frequently reduced to a confused mass of fine needles 
 which have extensively wandered out into the feldspar substance. The 
 ilmenite also is much crushed and elongated in the direction of the schist- 
 osity, but it shows no indication of being changed to leucoxene. 
 
 The second specimen, No. 11720, is somewhat schistose, though less 
 so than the last. It is extremely dark in color owing to the large pro- 
 portion of iron which enters into its composition. Under the microscope 
 it is a confused aggregate of very dark green and strongly pleochroic 
 hornblende needles, a little feldspar, proportionately much ilmenite and 
 quartz. Some of the larger hornblende crystals show the peculiar granu- 
 lated center, lately described and figured by me from the gabbro-diorites 
 occurring near Baltimore, 1 to which indeed this specimen presents many 
 points of close resemblance. 
 
 The two remaining specimens are much more altered than those just 
 described. 
 
 No. 11661, found beside the granite boss (the so-called “gold mine”) 
 just west of Pine street, Marquette, is coarsely granular. The feldspar 
 is altered to saussurite or calcite. The hornblende is pale green and 
 partly fibrous. The center of the crystals is frequently composed of a 
 dark, yellowish green substance which hardly polarizes at all. This, at 
 first glance, appears to be a core of compact brown hornblende but a 
 closer examination shows that this is not its nature. A little sphene 
 and considerable blood red iron hydroxide make up the remainder of 
 this rock. 
 
 The last specimen of these epidioritic rocks, No. 11711, was part of 
 a well marked dike of schistose greenstone which intersects a boss of 
 gneiss near the northern end of the Brook section. This gneiss strikes 
 E. and W., while the dike strikes N. 75° E. The schistosity of the 
 latter is parallel to its walls, so that the foliations of the two rocks 
 intersect at an angle. This rock shows the effects of pressure and 
 crushing. It is now a finely granular aggregate of pale green fibrous 
 hornblende, feldspar, quartz, calcite, and leucoxene. 
 
 1 Bull. TJ. S. Geol. Survey, No. 28, p. 28, PI. Ill, fifc. 1. 
 
 Bull. 62 10 
 
146 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 Diorite . — The occurrence of typical original diorite in the Marquette 
 area still seems a little doubtful. No. 11654, which composes the Picnic 
 Islands, a short distance north of Lighthouse Point, comes nearest to 
 deserving this name, although this rock might with as much propriety 
 be termed an amphibole granite. Julien called it a u quartzose porphy- 
 ritic diorite,” 1 and he was followed by Wadsworth. 2 The microscope 
 shows this rock to be a coarsely granular aggregate of green horn- 
 blende, saussuritized plagioclase, together with a less altered, unstriated 
 feldspar, quartz, and sphene. The hornblende is mostly quite com- 
 pact, and shows in cross-section sharp crystalline outlines, which are 
 often twinned. The plagioclase contains large zoisite individuals aside 
 from its more usual saussurite aggregate. The unstriated feldspar 
 seems to alter to muscovite or kaolin, as is common in orthoclase. 
 Seams in this rock are filled with epidote, calcite, or more rarely specu- 
 lar iron. 
 
 The Picnic Island rock seems to be most closely related to the amphi- 
 bole-granites, gneisses, diorites, and massive hornblendite which occur 
 in the granite farther north — notably on Partridge or Middle Island, 
 beyond Presqu’ Isle. At this latter locality there is every evidence, 
 from the intimate association of the granite and these hornblendic 
 rocks, that they were both liquid, or at least plastic, at the same time. 
 Such a perfect intermingling of the two magmas it seems impossible 
 to explain on any other hypothesis ; nor, indeed, are indications of the 
 same intermingling wanting on some of the Picnic Islands. 
 
 ACID INTRUSIVES. 
 
 General character . — The association of acid rocks of various types 
 with the greenstones of the northern portion of the Marquette area is 
 not less intimate than that already described as occurring at Upper 
 Quinnesec Falls, on the Menominee Eiver. (Chap. Ill, p. 110.) The 
 general character of these rocks is very similar at both localities, and 
 at both they offer equally valuable material for the study of dynamic 
 metamorphism. 
 
 The passage from the Marquette greenstones to the granite lying 
 north of them is an extremely gradual one. There is no such sharp 
 line of contact as is represented on RomingePs map, but, on the con- 
 trary, as Rominger himself explains, there is a complete interpenetration 
 of the two rock masses. The granite has intruded itself into the schis- 
 tose greenstones, for the most part following their bedding and forcing 
 apart their strata. The amount of the acid rock gradually diminishes 
 as we go southward. At the Dead River it still composes over half 
 of the entire mass, but between this and the city of Marquette the 
 dikes and bosses of granite grow less and less frequent. They are, 
 
 •Geol Mich., vol. 2, p. 163. 
 
 2 Notes on the Iron and Copper Rocks of Lake Superior. Bull. Mus. Comp. Zool., Harvard Coll. 
 Whole Series, vol. 7, Geol. Series, vol. 1, p. 39. 
 
WILLIAMS.] 
 
 THE GRANITE OF DEAD RIVER. 
 
 147 
 
 however, never entirely absent from the northern part of the green- 
 stone area, but extend to the limits of the Eureka series. Around 
 Lighthouse Point and near the Marquette water- works, on the north 
 side of the harbor, bands of reddish and gray acid rocks may be seen 
 along the lake shore in abundance. Some of these are but little altered 
 granites and porphyries, while others are decidedly schistose and seem 
 to owe their structure to dynamic agencies. 
 
 Granite . — We will first examine specimens of the unaltered granitic 
 type. These can be nowhere better seen than in the neighborhood of 
 the powder mill on Dead River, near the center of Section 10. Near 
 this place were obtained Nos. 11612 and 11613, both normal granites 
 which penetrate the schistose greenstones. They are of a reddish 
 color and consist principally of feldspar and quartz, both of which are 
 allotriomorphic and form a granular aggregate of interlocking grains. 
 The quartz areas are often composite, and are traversed by lines of 
 fluid-cavities, containing movable bubbles, The feldspar is both mon- 
 oclinic and triclinic. It is considerably altered to muscovite or kaolin. 
 A little chlorite represents the original presence, in small quantity, of 
 a third constituent, but its condition is now too much altered to allow of 
 its exact determination. The second of the two specimens (No. 11613) 
 is the coarser grained and contains both microcline and pyrite, which 
 are lacking in the former. 
 
 No. 11668, also from near the powder mill, occurs where the granite 
 and schistose greenstones are very intimately associated and it seems 
 to be intermediate between them. Under the microscope it appears as 
 a reddish granite, like those last described. Apatite crystals and mi- 
 nute, sharply defined zircons are abundant. The greenish color, which 
 imparts to this rock an appearance intermediate between a granite and 
 a greenstone, is due to the large amount of chlorite present. This 
 sometimes traverses the feldspar in irregular veins and is sometimes 
 massed together in larger areas, as though it had resulted from the al- 
 teration of some bisilicate, or, as is still more probable, of a micaceous 
 constituent. 
 
 Toward the southern end and on the west side of the Brook section, 
 the banded greenstones and granite are exposed in relations not less 
 interesting than those to be seen at Dead River. A large, glaciated sur- 
 face of the schists shows intrusions of both granite and diabase which 
 cut directly across the strike. The former rock contains angular frag- 
 ments of the schist and in one case it fills the inequality formed by the 
 faulting of the schist along a joint plane nearly perpendicular to its 
 bedding. It also forms narrow veins and rows of bulging lenses in the 
 schist. This granite shows no signs of foliation in the field, but a closer 
 study of it in the laboratory discloses the effects of powerful dynamic 
 action. The hand-specimen, No. 11678, proves upon microscopical ex- 
 amination to be an excellent example of peripheral granulation, pro- 
 ducing whatTornebohm has called the u mortar-structure.” The grains 
 
148 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 have rubbed against one another and formed a fine mosaic— mostly a 
 new crystallization — which resembles a cement. The quartz has suf- 
 fered so much by this process that hardly a trace of the original granitic 
 quartz remains. The feldspar presents rounded grains, often bent or 
 fissured. In the cracks thus formed the same mosaic-like cement is 
 developed. Chlorite, epidote, muscovite, and iron hydroxide are present 
 in this fine grained mass between the rounded feldspars. 
 
 No. 11710 was obtained from the rounded knob of gneissoid granite, 
 near the northern end of the Brook section, through which the dike of 
 foliated trap described on p. 145 (No. 11711) passes. In this rock the 
 gneissic structure is quite prominent through a parallel arrangement of 
 the constituent minerals, but under the microscope it quite closely re- 
 sembles the last specimen. The same peripheral granulation of the 
 original graius by rubbing is even more apparent ; and, although there 
 is no marked tendency to parallel arrangement visible in the thin sec- 
 tion, the effects of pressure are everywhere shown, as in the undulatory 
 extinction of the quartz, in the production of secondary strain-lamellae 
 in the feldspar, and in the presence of microcline. 
 
 No. 11614 was obtained from a gray granitic knob on the lake shore 
 at the mouth of Dead River. This is penetrated by several sharply 
 defined dikes of fine grained diabase, and, like the rock last described, 
 is decidedly gneissoid in structure. The rock is composed mainly of 
 quartz and orthoclastic feldspar, although both plagioclase and a green 
 fibrous hornblende are also present. The gneissic or u flaser ” structure 
 is its most striking feature. This is plainly visible in the thin section 
 and seems to be mainly due to the elongation of the quartz areas in 
 the direction of the foliation. This mineral has suffered greater defor- 
 mation than the feldspar and is present in long, lenticular patches* 
 whose axes are often sinuous. These are for the most part composite 
 and always show an undulatory extinction. There is, strangely enough, 
 no peripheral granulation visible in this rock. 
 
 No. 11660 is from a granite boss on the west side of Pine street, north 
 of Ohio street, Marquette. A fine section has recently been laid open 
 through the center of this mass by some eager gold seeker. The rock 
 is a fresh, even grained aggregate of orthoclase and quartz. Any origi- 
 nal micaceous constituent seems to be lacking, although good-sized 
 plates of muscovite have been secondarily developed at the expense of 
 the orthoclase. This feldspar possesses a beautiful zonal structure, 
 which is brought out in unusual distinctness by the different degrees to 
 which the alteration has progressed in different zones. The eruption of 
 this rock must have taken place subsequently to the dynamic move- 
 ments which metamorphosed so many of the Marquette intrusives. It 
 shows no evidence of pressure in its microscopic structure, although 
 No. 11658, collected but a few feet north of it, from a narrow baud of 
 acid rock, shows such evidence in a very marked degree. 
 
 Quartz porphyries .— No rocks are better suited to exhibit the effects 
 
WILLIAMS. J 
 
 QUARTZ PORPHYRIES AT MARQUETTE. 
 
 149 
 
 of dynamic metamorphism than the quartz porphyries. Some of the 
 more important results which this class of rocks has yielded to Euro- 
 pean students have already been stated in Chapter I. Near Marquette 
 the narrower of the dikes and intrusions of granitic matter have, in 
 consequence of their rapid cooling, assumed this form. Almost every 
 variety of structure between a typical granite and quartz porphyry 
 may be found by comparing specimens from the different exposures. 
 Furthermore, the various dikes seem to have been subjected to differ- 
 ent degrees of mechanical action, so that the successive phases of meta- 
 morphism may be traced by a comparative study of them. 
 
 In No. 11629 we have a granitoid porphyry which has suffered much 
 from chemical, but very little from mechanical alteration. This was 
 collected from a branching dike of a massive, reddish rock, exposed on 
 the lake shore near the water- works in Marquette. It approaches a 
 granite in being largely composed of porphyritie feldspar crystals with 
 but comparatively little interstitial groundmass. What there is of this 
 groundmass consists of a fine granular mosaic of quartz and feldspar 
 grains with some sericite. The larger feldspar crystals are colored red 
 by an abundance of fine globulitic dust. They also show an advanced 
 stage of chemical alteration in the development in them of a micaceous 
 mineral (sericite). The only traces of the original biotite consist of 
 chlorite areas dotted over with iron hydroxide. At first glance this rock 
 seems to resemble No. 11678 (above described as a fine example of 
 Tornebohm’s mortar structure), but a closer examination shows that the 
 structures, apparently so much alike, must have been produced by very 
 different means. There is in the present instance no evidence of press- 
 ure, the feldspar crystals have their original outlines intact, and the in- 
 terstitial mosaic, instead of being due to a grinding action between the 
 grains, is here evidently a product of the original crystallization. 
 
 The next specimen, No. 11620, is a typical quartz porphyry which also 
 has been but little modified by the effects of pressure. It is from a 
 small dike at the eastern extremity of Lighthouse Point and is a much 
 fresher rock than the last. The porphyritie crystals are both smaller 
 and less frequent. They consist of oi thoclase, plagioclase, and quartz, 
 imbedded in an abundant inicrogranitic groundmass. The ortlioclase 
 often shows a twinning structure in accordance with the Carlsbad law 
 and is extensively altered to muscovite, large plates of which occur 
 around its crystals. The quartz does not here possess its characteristic 
 dihcxahedral form, but occupies oval or irregularly shaped areas which 
 are frequently composite. 
 
 These two specimens will serve as representatives of those acid dike- 
 rocks which have been least modified by pressure. They will serve as 
 a starting point for tracing the successive stages of this action in the 
 following specimens. The changes observed are : The deformation and 
 elongation of the quartz crystals; the fracturing and separation of the 
 fragments of feldspars; the parallel arrangement of the new crystalliza- 
 
150 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 tion products, giving rise to a gneissic or “flaser” structure; and the 
 development of a cleavage. The intensity of these changes is of course 
 proportionate to the amount of force exerted. 
 
 No. 11633, obtained from the quarry on Lighthouse Point (A of map, 
 PI. VII), is a quartz porphyry which differs ouly slightly from No. 11620, 
 last described. Its groundmass is somewhat finer grained and sericitic. 
 The porphyritic crystals of feldspar are nearly the same, but the quartzes 
 are deformed and lenticular, sometimes with only an undulatory extinc- 
 tion, sometimes broken into several areas which are more or less dis- 
 placed from their original position. Although the thin section shows 
 no indications of schistose structure, this in the field is quite pronounced. 
 The rock occurs in the green schist, in small bands, which wedge out 
 very soon. It has a decided tendency to break along planes parallel to 
 the schist-bedding, and upon these planes of parting sericite is abun- 
 dantly developed. 
 
 No. 11653, from the northern edge of Lighthouse Point, just below the 
 Lighthouse, is very similar to the last, except that here a schistose 
 structure is microscopically, as well as macroseopically, visible. The 
 groundmass and porphyritic crystals are quite identical with those 
 above described. In the former there is a brown mica abundantly de- 
 veloped in aggregations of little plates, which form sinuous lines around 
 the porphyritic crystals in a direction parallel to the strike of the sur- 
 rounding greenstone schists. This fact is mentioned by Dr. Wadsworth, 
 who was the first to discover these rocks. 1 
 
 Nos. 11707 and 11717, were collected from two dikes of porphyry inter- 
 laminated with the green schists of the Brook section. In the hand speci- 
 mens they exhibit no marked foliation, but under the microscope their 
 evidences of mechanical alteration are most interesting and instructive. 
 The groundmass is of the same character as that already described. 
 In it, however, are sinuous bands of green mica which bend and wind 
 about the porphyritic crystals so as to produce a decided u micro-flaser” 
 structure. This feature is more pronounced in the second specimen, 
 although the two are essentially the same. The microscopic appear- 
 ance of 11707 is represented in PI. XV, fig. 2. The porphyritic feld- 
 spars have suffered little or no change, unless it be by the production 
 of microcline which is quite abundant in the center of some of the crys- 
 tals of No. 11707. The quartz has suffered much more deformation — 
 a fact which the observations of J. Lehmann 2 and Oh. E. Weiss 3 
 would indicate to be the rule in rocks of this character. In the present 
 case the quartz is drawn out into long, spindle shaped lenses which are 
 often pinched at their ends into fine lines that bend around the other 
 porphyritic crystals (see PI. XV, fig. 2). This deformation, however, 
 
 •Notes on the Iron and Copper Rocks of Lake Superior. Bull. Mus. Comp. Zool., Harvard Coll. 
 Whole Series, vol. 8, Geol. Series, vol. 1, p. 38. 
 
 2 Untersuchungon ilber die Entstehung der altkrystallinischen Schiefergesteine. Bonn, 1884. 
 
 3 Zeitsehr. Deutsch. geol. Gesell., vol. 29, 1877, p. 418, and Jahrbuch preuss. geol. Landesanstalt fur 
 1883, p. 213. Cf. Rosen busch: Mikros. Physiog., 2d ed., vol 2, 1887, p. 412. 
 
WILLIAMS.] 
 
 TUFFS OF THE QUARTZ PORPHYRIES. 
 
 151 
 
 does not take place without the loss of continuity in the quartz sub- 
 stance. On the contrary a mosaic-like aggregate of interlocking grains 
 is formed whose optical orientation differs more and more in proportion 
 as the original quartz crystal is elongated. In cases where the deforma, 
 tion is slight, only a disturbed extinction results, as may be seen in Ho. 
 11753. The presence of interlocking grains of different orientation, as 
 in this instance, would indicate solution and subsequent deposition. 
 
 Ho. 11658, from a narrow acid band immediately north of the granite 
 boss near Pine street, Marquette, is a rock of precisely the same type as 
 those just described but which shows a secondary schistose structure 
 more perfectly developed than any of the preceding. The brownish or 
 greenish mica is here arranged in nearly parallel bands which bend 
 only slightly around what were once porphyritic feldspar crystals. 
 These latter have undergone an almost complete change to muscovite 
 and quartz aggregates, some of which are now drawn out into long len- 
 ticular areas. These patches are hardly to be distinguished from the 
 groundmass, except by their coarser grain, and yet they can be traced 
 with certainty back to the original orthoclase. Sharp crystals of pyrite 
 and some epidote are also developed in this rock. 
 
 Tuffs of the acid rocks . — Closely allied to these schistose porphyries 
 which occur in dikes are certain banded acid rocks whose most impor- 
 tant exposures are along the southern edge of the northern Marquette 
 greenstone area, near the junction of this with the fissile argillaceous 
 shales of the “ Eureka series.” These are hard, compact, fine grained, 
 but decidedly schistose beds, locally known as novaculite. Indeed, 
 these rocks have been worked to a limited extent as whetstone, whence 
 the name of the small creek flowing through the southern part of Mar- 
 quette. 
 
 The color of these so-called novaculites is sometimes reddish, some- 
 times pale greenish or yellowish. They are very frequently stiiped with 
 different shades. Under the microscope they closely resemble the 
 groundmass of the quartz porphyries described in the last section. Ho 
 porphyritic crystals, however, are ever observed, and the structure is 
 too fine grained to appear schistose in a thin section. 
 
 Three essentially identical sections of these rocks were studied from 
 specimens collected at three of the most typical exposures. 
 
 Ho. 11627 is from near Burgess’s saw-mill, at the east end of Lake 
 street, Marquette. It has a reddish color produced by an abundance of 
 iron hydroxide scales. The grain is for the most part quite regular, 
 although larger and angular quartz fragments are occasionally seen. 
 
 Ho. 11684 was taken from the glaciated exposure of the novaculites, 
 occurring at the west end of Ridge street, Marquette. A fresh fracture 
 in this rock shows a light gray color. It is parted by intersecting joint 
 systems into sharp rhomboidal prisms which strike slightly south of 
 west. Under the microscope this rock appears as a fine, even mixture 
 of quartz grains and sericite flakes. 
 
152 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62 . 
 
 No. 11676 was collected at the south end of the “ Brook section,” 
 near Steinbrecher’s house. (B of map, Plate VII.) It is quite similar 
 to the others, but it is much seamed with infiltrated quartz, small veins 
 of which appear in the microscopic section. 
 
 The regular banding of these anomalous acid rocks, as well as their 
 interstratification with and gradual passage into the similarly banded 
 greenstone schists, will not admit of the supposition that they wereever 
 eruptive masses, however much we may imagine these to have been 
 metamorphosed. On the other hand, their similarity, in both composi- 
 tion and structure, to the groundmass of the quartz porphyries, is too 
 striking to be overlooked. 
 
 Apparently only two hypotheses are altogether reconcilable with the 
 observed facts : First, that the rocks are true sediments, like those of 
 the Eureka series, along whose northern edge they lie, which may have 
 been largely derived from disintegrated quartz porphyry material ; or 
 second, that they are consolidated acid tuifs which accompanied the 
 eruptions of the porphyries, in the same manner that some of the 
 greenstone schists represent the fragmental diabase material. 
 
 Another possible supposition is that these compact, hornstone-like 
 rocks resulted from the contact-metamorphism of preexistent sediments 
 by the diabase eruptions. Such an effect has been extensively pro- 
 duced by the Hartz Mountain diabase, as has been shown by the work 
 of Lossen and others. The resultant rock is known as adinole , but 
 it differs essentially from the Marquette novaculite in a constant and 
 high percentage of soda, due to the presence of albite. This, as may 
 be seen from the following analysis, is absent from the Marquette rock. 
 We further have no evidence of the existence of sediments when the 
 greenstones were produced, as all the Huronian beds are younger. 
 
 Of the two first mentioned hypotheses, the second is the more proba- 
 ble, first, because of the very constant character of these banded acid 
 rocks, and second, because of their almost exact identity in chemical 
 composition with the massive acid eruptives. The following chemical 
 analysis of specimen No. 11681, from the west end of Ridge street, Mar- 
 quette, was made by Mr. W. F. Hillebrand : 
 
 Silica (Si0 2 ) 
 
 ... 76.99 
 
 Potash (K 2 0) , 
 
 3. 65 
 
 Alumina (A1 2 0 3 ) 
 
 ... 13.92 
 
 Soda (Na 2 0) 
 
 0. 56 
 
 Ferric oxide (Fe 2 03 ) 
 
 0.45 
 
 Lithia (Li 2 0) 
 
 Trace. 
 
 Ferrous oxide (Fe 0) 
 
 0.77 
 
 Water (H 2 0) 
 
 2. 35 
 
 Manganous oxide (MnO) 
 
 Lime (CaO) 
 
 Magnesia (MgO) 
 
 ... Trace 
 
 Phosphorous pentoxide (P 2 0 5 )... 
 
 Trace. 
 
 
 Total 
 
 100. 13 
 
 It will be seen that this is the composition of an aggregate of quartz 
 and sericite, as the microscope shows our novaculite to be. The sericite 
 is in all probability the result of the alteration of original orthoclase. 
 
 The occurrence of similar tuff deposits in connection with eruptive 
 quartz porphyries is well known in Europe, especially in the German 
 
WILLIAMS.] 
 
 ACID TUFFS FROM OTHER LOCALITES. 
 
 153 
 
 dyas. They have been carefully studied and described in Saxony , 1 the 
 Yosges Mountains , 2 the Black Forest , 3 and Odenwald . 4 The writer can 
 speak from a very considerable personal acquaintance with the Black 
 Forest and Odenwald tuffs, of their very close resemblance to the Mar- 
 quette novaculites. 
 
 But perhaps the closest analogues of the Marquette tuffs are to be 
 found among those described by Dr. Archibald Geikie, from St. David’s, 
 in Wales , 5 a region which, as we shall see in the sequel, presents many 
 points of resemblance to the Marquette district. The analysis of one of 
 them, hereafter quoted (Y), agrees very closely with that of our novac- 
 ulite. Dr. Geikie finds that these acid tuffs accompanied superficial 
 eruptions of quartz porphyries, which were intimately associated with 
 more abundant and contemporaneous extrusions of diabase and diabase 
 tuffs. The acid tuffs have been derived from true fine grained felsites. 
 Some of them are conglomeratic (agglomerates); some of them fine ashy 
 material, which has become consolidated into a sericitic schist. There 
 are various intermediate varieties between the acid and basic types, 
 due to the mingling in different proportions of the two kinds of debris. 
 
 Mr. J. S. Diller 6 has also shown that the felsitic rock from Breakheart 
 Hill, near Saugus, Massachusetts, is a silicified quartz porphyry tuff; 
 and from the sharply angular shape of the quartz fragments, of which 
 it is now composed, he concludes that these are pseudomorphs after 
 fragments of an acid glass originally deposited as a volcanic ash. 
 
 The following analyses of well characterized acid tuffs from European 
 localities are here quoted on account of their similarity to the Mar- 
 quette novaculite : 
 
 
 I. 
 
 II. 
 
 III. 
 
 IV. 
 
 V. 
 
 Silica (Si0 2 ) 
 
 Alumina (AI 2 O 3 ) 
 
 Ferric oxide (Fe 2 0 3 ) > 
 
 Ferrous oxide (FeO) > 
 
 Lime (CaO) 
 
 76. 37 
 13. 94 
 
 3.18 
 
 79. 73 
 11.34 
 
 0.99 
 
 82. 47 
 9. 55 
 c 0.43 
 l 0.57 
 0. 53 
 trace . . . 
 4.69 
 0.58 
 1.18 
 
 84. 12 
 9. 38 
 
 | 1.78 
 
 0 . 08 
 0.01 
 0. 85 
 0. 25 
 3. 68 
 
 80.59 
 11.29 
 r 0.28 
 
 l *1. 41 
 0.52 
 0.95 
 2. 98 
 0. 72 
 tl.96 
 
 Magnesia (MgO) 
 
 Potash (K 2 0) 
 
 Soda (Na^O) 
 
 Water (H 2 0) 
 
 Total 
 
 4.39 
 1.07 
 1. 58 
 
 0.27 
 3.81 
 0. 17 
 2. 12 
 
 100. 53 
 
 98. 43 
 
 100. 00 
 
 100. 15 
 
 100. 70 
 
 * Manganous oxide trace. tLoss on ignition and water. 
 
 1 C. F. Naumann: Geognosie, 2d ed., vol. 1, p. 671,1858. Also Erlauterungon zur geol. Specialkarte 
 des kon. Sachsens, Sect. Frohburg (59), Colditz (44), Dobeln (46), Leisnig-Lausigk (43), and Rochlitz 
 
 (60). 
 
 2 D. Gerhard : Geognistisch-petrographische Mittheilungen aus dem Gebweiler-Thal, 1880. (Cf. Noues 
 . Jabrbucb fur Mineral., 1881, vol. 1 , Referate p. 374). 
 
 ‘‘G. H. Williams: Neues Jahrbuch fiir Mineral., Boilage-Band 2, pp. 626-634. 
 
 4 Benecke and Cohen : Geogn. Beschr. d. Umgegend von Heidelberg, 1881. pp. 221-235. 
 
 6 On the supposed pre-Cambrian rocks of St. David’s. Quart. Jour. Geol. Soc. London, vol. 39, pp. 
 298-301, 1883. 
 
 r, The felsites and their associated rocks north of Boston. Proc. Bost. Soc. Nat. Hist., vol. 20, pp. 
 365-368; Bull. Mus. Comp. Zool., Harvard Coll. Whole Series, vol. 7, pp. 165-180; also Science, 1884. 
 vol. 3, p. 653. 
 
154 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 I. Thonstein (tuff) from Zeisigwald, near Chemnitz, Saxony. 1 
 
 II. Same. 2 
 
 III. Silicified tuff, Oelberg, near Schriesheim, Odenwald. 3 
 
 IV. Silicified tuff, Kesselberg, near Triberg, Black Forest. 4 
 
 V. Felsitic tuff breccia, Clegyr Hill, St. David’s, Wales. 5 
 
 If, then, these banded acid rocks occurring near Marquette, as seems 
 most probable, really do represent solidified, tuff material of the quartz 
 porphyries, we might expect to find transitional forms, grading into the 
 banded green schists. These do appear to exist, and indicate that 
 some, at least, of the eruptions of both acid and basic rocks were nearly 
 contemporaneous. 
 
 BANDED GREENSTONE SCHISTS. 
 
 The banded greenstone schists which form the prevailing rock over the 
 northern portion of the Marquette area have been regarded by all geolo- 
 gists who have ever studied them as originally sedimentary deposits, 
 and a repeated examination of them in the field seems incapable of 
 leading to any other conclusion. They are everywhere stratified with 
 the greatest regularity in bands of lighter and darker shades of green. 
 This structure is to be most advantageously seen in the woods just 
 north of Marquette and near Lighthouse Point. Here glaciated areas 
 of considerable extent often show a finely ribboned appearance, looking 
 as though the sharp, parallel lines had been drawn with a ruler. The 
 alternation in the color and composition of the layers is so frequent and 
 so constant, and their parallelism to the east and west strike of all the 
 rocks of this neighborhood is so exact that no hypothesis of their orig- 
 inally massive character will satisfactorily account for the observed 
 facts. 
 
 On the other hand, the chemical and the microscopical characters of 
 these schists agree closely with those of associated massive greenstones 
 which are known to have been derived by the alteration of basic erup- 
 tive rocks. Both are composed of fibrous green hornblende, quartz, 
 epidote, zoisite, and chlorite. There must, therefore, have been a close 
 similarity in the original composition of these two classes of rocks, in 
 spite of the wide difference in their structure. 
 
 Prof. M. E. Wadsworth, who has ably advocated the eruptive origin 
 of many of the rocks occurring near Marquette, regards these banded 
 schists as undoubtedly of sedimentary origin. He says : 6 
 
 The schist from the same specimen (45) is composed of quartz, argillaceous mate- 
 rial, chlorite, hornblende, magnetite, “ leucoxene,” and a little augite. It would seem 
 that this had been formed from detrital material of the same nature as the dikes 
 (basaltic). The close resemblance of the “diorite” and schist in mineralogical char- 
 acters, but not in structure, is shown in another section containing the junction of the 
 two rocks (48). ^ . 
 
 1 Neues Jahrbneh fur Mineral., 1864. 
 
 2 Ibid., 1859. 
 
 3 Die zur Dyas gehcirigen Gesteino des siidlichon Odenwaldes, von E. Cohen, 1871, p. 57. 
 
 * Neues Jahrbuch fur Mineral., Beilage-Band 2, p. 630. 
 
 8 Quart. Jour. Geol. Soc. London, vol. 39, 1883, p. 297. 
 
 6 Notos on the Iron and Copper Districts of Lake Superior. Bull. Mus. Comp. Zool., Harvard Coll., 
 Whole Series, vol. 7, Geol. Series, vol. 1, p. 37. 
 
Williams. J SHEAF-LIKE HORNBLENDE IN THE BASIC TUFFS. 155 
 
 Specimes of these banded greenstone schists which were collected 
 from different localities within the northern Marquette area, although 
 they are macroscopically nearly identical, present a great variety in 
 their microscopical structure. 
 
 Nos. 11618 and 11619, from Lighthouse Point, Marquette, are com- 
 paratively coarse grained rocks composed largely of a green fibrous 
 hornblende. The structure of this mineral, especially in No. 11619, is 
 unusual. What at first glance looks like a confused mass of irregular 
 and ragged hornblende areas, when more carefully examined, is found 
 to consist of more or less radiating bundles of hornblende fibers, resem- 
 bling sheaves. The center of these bundles is their most compact por- 
 tion. Here the hornblende substance is often continuous and homo- 
 geneous, but toward the two ends of the mass it appears to be frayed 
 out into separate fibers. These are so regularly divergent in their ar- 
 rangement as to produce a black brush which sweeps across them as 
 the stage of the microscope is revolved between crossed Nicol prisms. 
 This peculiar, sheaf-like grouping of the hornblende is shown in PI. XVI, 
 Fig. 1. It is very similar to that described by de la Vallee-Poussin and 
 Renard in an amphibolite occurring near Laifour, in the valley of the 
 Meuse, 1 and by Renard in the metamorphosed Devonian slates of Bas- 
 togne in the Ardennes Mountains. 2 Though it can still be traced in 
 specimen No. 11618, this structure is by no means as distinct as in the 
 case just described. 
 
 The groundmass in which this hornblende lies is a finely granular 
 aggregate of albite, or quartz and albite grains. In it occur some 
 chlorite, epidote, or zoisite in good sized individuals, and, at least in 
 No. 11619, some small ilmenite particles, surrounded by a highly refrac- 
 tive leucoxene border. There is comparatively little groundmass in 
 either of these specimens, but of the two No. 11618 contains the more. 
 
 Nos. 11730, from the western part of Marquette, between Michigan 
 and Ohio streets, and 11734, from the corner of Front and Ohio streets, 
 are both banded greenstones of the same type as the specimens last 
 described. The former contains less hornblende, though this mineral, 
 is, nevertheless, abundant in the same sheaf like bundles as before. 
 The groundmass is a fine grained albite mosaic, which contains some 
 quartz and some epidote. The latter specimen, No. 11734, is largely 
 composed of an unusually dark green and pleochroic hornblende, in con- 
 fused ragged and fibrous groups. Along certain lines, where this compo- 
 nent is less abundant, the rock assumes a lighter shade. The albite mo- 
 saic is present, but not to the exclusion of areas of gray saussurite, 
 which sometimes show indications of a latli-like form, like that of the 
 diabase feldspars. Narrow seams filled with epidote, or an aggregate 
 of albite and epidote, traverse this rock parallel to its banding. Ilmen- 
 ite grains, with their rims of leucoxene, occur in each of these specimens. 
 
 *M6m. sur les char. min. et strat. des roches dites plutoniennes, etc., Brussels, 1876, p. 252, PI. V, 
 
 Fig. 25. 
 
 2 Les roches gr6natif6res et amphiboliques do la r6gion de Baatogno. Bull. Mus. roy. d’liist. nat. de 
 Belgique, 1882. 
 
156 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62. 
 
 There is nothing in the microscopical structure of these slides to sug- 
 gest a massive eruptive rock; on the contrary, the two instances cited, 
 where a similar sheaf like hornblende has before been noticed, are cases 
 of supposed metamorphosed tuffs. 
 
 No. 11630, from the quarry on Lighthouse Point (A of map, PI. YII) is 
 also largely composed of hornblende in pale green, ragged-looking indi- 
 viduals, but without any of the sheaf-like structure. Amid the horn- 
 blende a clear transparent feldspar, evidently albite, has been abund- 
 antly developed in good-sized grains, which show a sharp twinning stri- 
 ation. The gradation of this well characterized albite into the granu- 
 lar mosaic lends additional force to the supposition that this also is com- 
 posed of the same mineral, as, indeed, Lossen has shown to be the case 
 in many of the regionally metamorphosed diabases of the eastern Hartz. 1 
 
 Nos. 11631 and 11637 are other specimens of the banded greenstone 
 schists from the same quarry as the last on Lighthouse Point. The for- 
 mer is, perhaps, the most typical, although an abundance of calcite 
 shows that it is mueh weathered. Its alternating light and dark green 
 bands are due to the fact that hornblende is still present in the latter, 
 while its place is supplied in the lighter colored bands by a pale chlor- 
 ite and epidote. An opaque iron oxide, often surrounded by a leu- 
 coxene rim, is found in small particles scattered through this rock, as 
 is also a little biotite. The second of. the above mentioned specimens, 
 Np. 11637, which was taken from just beside the great dike, shows what 
 the last described rock was when it was in a fresher condition. The cal- 
 cite is here absent, and the rock is, for the most part, a mass of ragged 
 and raveled hornblende. Among this is scattered some clear, trans- 
 parent feldspar (probably albite) and zoisite, or epidote, which occurs in 
 irregular crystalloids, arranged in long, parallel lines. The iron mineral 
 and biotite are present as before. 
 
 No. 11623, found beside the great dike on Lighthouse Point, is only 
 a confused aggregate of very pale and very fibrous hornblende needles 
 with calcite. Lighter bands are occasioned in this rock by a prepon- 
 derance of calcite and chlorite over the hornblende. 
 
 No. 11626 is a gray schistose rock from the exposure near Burgess’s 
 saw mill, on Lake street, Marquette. It is full of calcite, which is ar- 
 ranged in bands along with a very finely granular mosaic. Hardly any 
 hornblende is visible in this specimen, but veins of epidote and some 
 chlorite occur in it. 
 
 Along the deep north and south exposure of the greenstone schists 
 which has been described as the Brook section, these banded greenstones 
 • are also very admirably displayed. For the most part they are qtfite 
 like those occurring in the neighborhood of Marquette. In one par- 
 ticular, however, some of them present an unusual feature which it is 
 not altogether easy to explain. This consists in the presence of len- 
 
 1 Zeitscbr. Deutsch. pool. GeselJ., vol. 24, 1872, p. 730. Jahrbucli preuss. geol. Landesanstalt fur 
 1883, p. 640; ibid., fiir 1884, p. 528. Eriaut. zur geol. Specialkarte von Pr., Blatt Wippra, Berlin, 1883. 
 
WILLIAMS.] WHITE AUGEN IN THE GREENSTONE SCHISTS. 157 
 
 ticular masses of a white feldspathic substance, which are so elongated 
 in the direction of the bedding that while they generally present a 
 lens-shaped form, their cross-section is nearly circular. The size of 
 these lenses, which externally resemble what the Germans call “Augen” 
 or eyes, is extremely variable. Some are smaller than peas, while others 
 are more than two inches in length. The extent also to which they are 
 elongated differs very much in different cases. Some are represented 
 only by narrow white lines which are occasionally thickened or swelled 
 out into oval spots. Between these and such as vary comparatively 
 little from a spherical form we may find all intermediate stages. 
 
 These white lenses are by no means universally distributed through 
 the green-schists of the Brook section; on the contrary they occur only 
 rarely in bands which transverse the greenstones parallel to their bed- 
 ding. One of these bands consisted of only a few rows of large, oval 
 masses, exactly resembling rounded pebbles, but in spite of its narrow- 
 ness it could be traced for a considerable distance. 
 
 The white color of these lenses or “Augen” presents a decided con- 
 trast to the dark green of the inclosing schists. Their outline, too, is 
 quite sharp, and yet, upon a close examination, they are seen to pass 
 gradually into the substance of the surrounding rock. What their 
 origin was, whether they were inclusions much flattened by subsequent 
 pressure, or secretions of the rock itself, or infiltrations, it now seems 
 difficult, if not impossible, to decide. 
 
 Sections 11703 to 11705a, show the microscopic composition and 
 structure of these lenticular masses as well as their relation to the in- 
 closing rock. This latter is in all cases a typical hornblende schist or 
 amphibolite. It is composed of small, compact needles of strongly 
 pleochroic, green hornblende, colorless grains of feldspar and probably 
 quartz, and the minute, highly refractive epidote particles so character- 
 istic of the crystalline schists. The feldspar is very fresh and free from 
 inclusions, as though it were the product of a new crystallization. It 
 rarely possesses an albite or microcline twinning structure, but for the 
 most part it is so homogeneous and limpid that it closely resembles 
 quartz. Lossen has called particular attention to the difficulty of dis- 
 tinguishing a mosaic of secondary albite from quartz under the micro- 
 scope, 1 and it is very possible that quartz grains are actually present 
 in this rock, although in certain favorable cases a biaxial character was 
 substantiated. 
 
 No. 11703 is cut in the direction of the bedding and shows the horn- 
 blende in strictly parallel arrangement. Its feldspar “Augen” are very 
 much elongated, while in No. 11705, which is cut nearly perpendicular 
 to the bedding, they are as broad as they are long. This substance 
 was undoubtedly once some triclinic feldspar, but this has been changed 
 to saussurite which now consists of epidote and sericite imbedded in a 
 
 1 Zeitschr. Deutscli. geol. Gesell., vol. 31, 1879, p. 441, et seq. Jahrbuch preuss. geol. Landcsanstalt 
 fur 1884, pp. 528, o44, PI. XXIX, fig. 4. 
 
158 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 IBULL. 62. 
 
 new crystallization of albite. They contain no hornblende, but there 
 seems to be a condensation of this mineral in the schist around their 
 edge and enough of it penetrates for a distance into their substance to 
 form a gradual transition rather than a sharp line of contact between 
 them and the inclosing rock. 
 
 The composition of these a Augen” is not in every instance the same, 
 although they all appear to have been derived from some form of 
 feldspar. In No. 11704 they are composed wholly of epidote, while in 
 No. 11705a the original feldspar was more acid and sericite has been 
 produced almost to the exclusion of epidote. 
 
 Other of the banded greenstones collected along the Brook section 
 are quite devoid of the white “Augen” and agree closely with the rocks 
 around Marquette. 
 
 Nos. 11706, 11713, and 11718 are essentially hornblende rocks, con- 
 taining some altered feldspar and some quartz. They are plainly 
 banded, the alternate layers differing in both color and composition. 
 
 No. 11671, from an exposure very near the center of section 17, con- 
 sists of sharp epidote needles and a little quartz, imbedded in a con- 
 fused mass of pale green, fibrous hornblende. 
 
 Nos. 11610, 11611, and 11667, from near the powder mill on Dead 
 Biver, are all schistose greenstones in a much altered condition consist- 
 ing now of chlorite, quartz, and carbonates. 
 
 As has been already remarked, the structure of these greenstone- 
 schists is such as to necessitate a belief in the original nature of their 
 stratification; while, on the other hand, their chemical as well as their 
 mineralogical composition renders it impossible to separate them from 
 the massive and highly altered greenstones (uralite diabases, etc.), 
 with which they are most intimately associated. Their parallel band- 
 ing indicates a fragmental, but their chemical and their mineral com- 
 position indicate an igneous origin. The only satisfactory reconciliation 
 of these opposite sets of characters is to be found in that group of 
 rocks intermediate between sediments and lavas, known as volcanic 
 tuffs. 
 
 In the opinion of the writer, then, the banded greenstone schists of 
 the northern Marquette area are to be regarded as consolidated and 
 highly metamorphosed diabase tuffs. These are intimately associated 
 with numerous contemporaneous flows of diabase and quartz porphyry, 
 together with tuffs of the latter rock ; while all have been broken through 
 by much younger dikes, both basic and acidic. 
 
 From the preceding petrographical descriptions it will be seen how 
 great is the similarity between the banded greenstones of Marquette 
 and the older massive diabases. Mineralogically, they are now iden- 
 tical, but the flue parallel banding of the former necessitates the 
 assumption that their origin differed from that of the eruptives. 
 
 In a former paper 1 the writer has maintained that two geological 
 
 1 Bull. U. S. Geol. Smvey, No. 28, p. 1. 
 
WILLIAMS.] 
 
 ORIGIN OF THE BANDED GREENSTONES. 
 
 159 
 
 masses as different in tlieir structure and origin as a clay-bank and a 
 lava-stream, if they possessed the same chemical composition to start with , 
 when subjected for a long period to exactly the same physical condi- 
 tions, would result in the same products. This is, of course, true only 
 when these conditions allow of profound metasomatic and structural 
 changes. On the other hand, when we find two intimately associated 
 rocks which for a long time have been subjected to exactly the same 
 conditions, but which still bear evidence of dissimilar origin, in spite of 
 practical identity of mineral and chemical composition, we may safely 
 consider them as originally of the same, or of similar chemical composi- 
 tion. Now, it is difficult to imagine any stratified sediments of the 
 composition of diabase, except diabase ashes j nor could these have un- 
 dergone transportation by water without suffering important chemical 
 changes. We therefore conclude that the banded schists represent vol- 
 canic debris deposited at or near the point of its origin. 
 
 In order to obtain a clear idea of just how these ancient and much 
 disguised tuffs acquired their present form and apparently dual char- 
 acter, it will be advantageous to ascertain what is known of analagous 
 formations of comparatively recent date. Capt. C. E. Dutton’s de- 
 scriptions 1 of the fragmental rocks accompanying the Tertiary erup- 
 tives of the high plateaus of Utah, are well suited to this purpose. He 
 says, in speaking of the extent of these deposits : 2 
 
 Some of the most interesting lithological problems presented by the volcanic prod- 
 ucts of the high plateaus are those relating to the origin and development of what 
 may be termed the clastic igneous rocks, or rocks apparently composed of fragmental 
 materials of igneous or volcanic origin, but now stratified either as so-called tufa- 
 ceous deposits or as conglomerates. These are exceedingly abundant in all of the 
 great volcanic districts of the world, and often enormously voluminous. How those 
 of the high plateaus would compare, in respect to magnitude, with those of other 
 regions, I do not accurately know, but absolutely their bulk is a source of utter aston- 
 ishment. They cover nearly 2,000 square miles of area, and their thickness ranges 
 from a few hundred feet to nearly 2,500 feet, the average being probably more than 
 1,200 feet. Lavas are frequently intercalated, but much more frequently no inter- 
 calary lavas are seen, and in general they seldom for any large proportion of the 
 entire bulk when they occur in conjunction with the clastic masses. 
 
 Again, in speaking of the peculiar liability of such deposits to meta- 
 morphism, the same writer says : 3 
 
 A very striking characteristic of these clastic volcanic rocks, both the tufas and 
 the conglomerates, is their great susceptibility to raetamorphism. Not oulv have the 
 beds in many localities been thoroughly consolidated, but they have undergone crys- 
 tallization. Those tufas and conglomerates which are of older date, and which have 
 been buried beneath more recent accumulations to considerable depths, rarely fail to 
 show conspicuous traces of alteration, and in many cases have been so profoundly 
 modified that for a considerable time there was doubt as to their true character. The 
 general tendency of this process is to convert the fragmental strata into rocks having 
 a petrographic facies and texture very closely resembling certain groups of igneous 
 rocks. When we examine the rocks in situ no doubt can exist for a moment that 
 
 1 Report on the Geology of the High Plateaus of Utah. By C. E. Dutton ; Washington, 1880. 
 
 * Ibid., p. 69. 3 ibid., pp. 79, 80. 
 
160 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 they are water-laid strata. The hand-specimens taken from the beds, which are ex- 
 tremely metamorphosed, might readily pass, even upon close inspection, for pieces 
 of massive eruptive rocks were it not that the original fragments are still distinguish- 
 able, partly by slight differences of color, partly by slight differences in the degree 
 of coarseness of texture. But the matrix has become very similar to the included 
 fragments, holding the same kinds of crystals, and under the microscope it shows 
 a groundmass of the same texture and composition. # * * 
 
 I see nothing at all incredible in the idea of metamorphism producing rocks so 
 closely resembling some eruptive rocks that they can not be petrographically distin- 
 guished from them. It seems rather that we ought to anticipate just such a result 
 from the alteration and consolidation of pyroclastic strata. The materials which 
 compose them consisted originally of disintegrated feldspar, pyroxene, and the mat- 
 ter which constitutes the amorphous base of all eruptive rocks. 
 
 We are thus enabled to see that there is, at least, no geological diffi- 
 culty in the explanation here offered of the origin and nature of the 
 banded green-schists at Marquette. On the high plateaus of Utah, 
 which form one of many similar districts, conditions are plainly seen 
 to have prevailed quite similar to those here assumed for the more 
 ancient rocks of Lake Superior ; and yet the metamorphism which has 
 taken place in the ancient Archean deposits is hardly greater than 
 that described by Captain Dutton in the tertiary tuffs. 
 
 The most generally accepted type of diabase tuffs is the German 
 “ Schalstein f but, as Rosenbusch well remarks , 1 in the course of many 
 years so many totally different rocks, with only the most superficial re- 
 semblance to each other, have been described under this designation, 
 that there is now no definite meaning whatever which can be attached 
 to this term. The schalsteins are for the most part, green or greenish 
 in color, earthy and schistose $ but among them have been included 
 altered and foliated diabases on the one hand, and true sediments on 
 the other, while some of them are undoubtedly true diabase tuffs. In 
 Germany their distribution is very wide in Nassau, Saxony, and Ba- 
 varia. 
 
 The microscopic sections of German Schalsteins accessible to me for 
 comparison were those in the Stiirtz collection of typical rocks belong- 
 ing to the petrographical laboratory of the Johns Hopkins University. 
 They are from the localities of Riibeland in the Hartz Mountains, and 
 Diez, Baldinnstein, Dillenburg, and Weilburg in Nassau. In spite of 
 extreme alteration, resulting in several cases in the survival of only 
 chlorite, calcite, and iron oxide, it can be distinctly seen that the speci- 
 mens were originally totally different. The rocks from Diez, Dillen- 
 burg, and two out of the three labeled Weilburg, are only very arnyg- 
 daloidal diabcses. The structure in the base is well preserved, while 
 the amygdules are filled with calcite surrounded by a rim of chlorite. 
 The rock from Riibeland is apparently of the same nature, but the origi- 
 nal structure has now disappeared. In the specimen from Baldinnstein 
 and m one from Weilburg there is no indication of diabase structure, 
 but there is a spheroidal aggregation resembling that seen in palagonite. 
 
 1 Mikros. Physiog. , 2d ed., vol. 2, p. 245. 
 
WILLIAMS.] 
 
 FOREIGN DIABASE TUFFS. 
 
 161 
 
 The most extended descriptions of these rocks have been given by Gum- 
 bel, who has treated the schalsteins of the Fichtelgebirge in Bavaria in a 
 most careful manner. 1 Rothpletz has described the tuffs and agglom- 
 erates associated with the Silurian diabases in Saxony. 2 In Great 
 Britain the ancient volcanic areas of Cornwall and St. David’s in Wales 
 show the closest similarity, both in the character of their rocks and in 
 certain features of their structure to the Marquette region. The slaty 
 blue u eivans ” of the former district were regarded by De la Beche as 
 altered ash-beds. 3 J. Arthur Phillips arrived at the same conclusion. 4 
 He says : 
 
 The Coruish rocks afford numerous examples of ancient lava flows so interbedded 
 with slates and schists of the district as to lead irresistibly to the conclusion that 
 they are contemporaneous ingeous deposits. 
 
 Also again : 5 
 
 The slaty blue eivans found between St. Erth and St. Stephens (in Bramwell) have 
 a chemical composition identical with that of the altered dolerites, and may be, as 
 was formerly suggested, highly metamorphosed ash-beds. 
 
 The basic tuffs, like the acid ones, occurring at St. David’s have been 
 described by Dr. A. Geikie. 6 He finds that all varieties of texture can 
 be traced, from large grained breccias to fine schistose mudstones. The 
 finer material includes angular, subangular, and rounded blocks or 
 lapilli, consisting not alone of diabase, but also of the more acid felsitic 
 rocks. These are true agglomerates, and their striking resemblance to 
 certain other of the schistose greenstones of the Marquette belt will 
 be alluded to in the sequel. 
 
 • The eruptive rocks which Dr. Hans Beusch has recently studied in 
 the regionally or dynamically metamorphosed district on the west coast 
 of Norway, present a close resemblance to those occurring near Mar- 
 quette. 7 He finds diorites, in part very schistose, which have originated 
 through the metamorphism (uralitization and epidotization) of ancient 
 
 1 Geognostisclie Beschreibung ties Fichtelgebirges, mit dem Frankenwald und dem westliclien Vor- 
 lande, Gotha, 1879, pp. 222 et seq. 
 
 2 Erl. zurgeol. Specialk. Sachsens, Sect. Frankenberg-Hainichen(78), j>p. 16 and 21 ; Sect. Sekellenberg- 
 Floka (97), p. G». 
 
 3 Geological Observer. 
 
 4 Quart. Jour. Geol. Soc. London, vol. 34, p. 493. 
 
 5 Ibid, p. 495. 
 
 6 Quart. Jour. Geol. Soc. London, vol. 39, p . 297, 1883. 
 
 7 Geologische Beobachtungen in einem regional-metamorphosirten Gebiet am Hardangorfjord in 
 Xorwegen, Neues Janrbuchfiir Mineral., Beilage-Band 5, pp. 52-67. On pages 54, 55 the author says: 
 Nicht selten zeigt das dioritische Gestein einen schichtenweisen Weehsel von verschiedonen Varie- 
 taten. In diesem Falle bin ich geneigt, anzunehmeu, dass das urspriingliche Gestein nach Art der 
 Tuffegebildet wurde. Dies geschichtete dioritische Gestein bildet einen Uebergang zuden griinlickeu 
 feinkbrnigen oder dichten, geschichteten, mehr oder weniger schieferigen Gesteinsarten, wolclie die 
 Hauptmasso von dem ausmachen, was ich fur basische Tuffe halte. Diese Gesteine fiihren ala woscnt- 
 licho Bestandtheilo Hornblende, Chlorit und Epidot, daueben gem roichlich Carbonspath. Sie ent- 
 sprechen eiuigermassen den Schalsteinen der deutschen Petrographen. Eingelagert kommen Masson 
 vor, die man am ehesteu fiir geflossene Strbmo lialten muss. Einige Bind wohl auch intrusive Gaugo. 
 Uebrigens ist es hier, wie anderswo unter ahnlichen Verhiiltnissen, oft schwierig zu untorscheiden 
 was massig erstarrtund was klastischo Bildung ist. For the detailed descriptions of these rocks by 
 Dr. Reusch, see “Bommelben og Karmben,” Christiania, 1888 (in Danish), p. 112, and the appended 
 ‘ English summary of contents, p. 402. 
 
 Bull Gli 11 
 
 |M|M 
 
162 
 
 GREENSTONE SCHIST AREAS OP MICHIGAN. 
 
 [BULL 62. 
 
 gabbros. These are most intimately associated with granites and quartz 
 porphyries, while both acid and basic rocks are accompanied by abun- 
 dant tuff deposits. 
 
 In America hardly anything reliable has been published on basic tuffs. 
 Edward Hitchcock speaks of diabase tuffs in the trias of Massachu- 
 setts, but gives nothing specific respecting their nature . 1 References 
 to this class of deposits are scattered through the writings of some of 
 the Canadian geologists, especially in the recent report of Mr. A. C. 
 Lawson on the Lake of the Woods region . 2 
 
 1 Geology of Massachusetts, 4°, 1841, p. 648. 
 
 2 Geol. and Nat. Hist. Survey Canada, Ann. Kept, for 1885, Kept. CC., 1886. 
 
 . 
 
GREENSTONE BELTS OF THE MARQUETTE DISTRICT— Continued. 
 
 ROCKS OF THE SOUTHERN PORTION OF THE MARQUETTE AREA. 
 
 On the south side of the narrow band of Huronian slates which has 
 been designated as the w Eureka Series,” the greenstones of the Mar- 
 quette area present a decided contrast to those which have been 
 described in the previous section as occurring on its north side. They 
 are, for the most part, massive, pale green in color, and apparently 
 homogeneous in structure. Only in rare instances can individual min- 
 erals be detected with the unaided eye. A schistose structure is not 
 uncommon in these rocks, but it is evidently a pressure foliation, while 
 the parallel banding or striping, so frequent in the greenstones of the 
 northern area, is altogether absent. A study of these pale green 
 aphanitic greenstones seems to indicate that they were not originally 
 to any great extent tuff deposits, but massive flows of diabase, which 
 have since suffered profound chemical and structural change in conse- 
 quence of having been subjected to intense dynamical action. 
 
 In addition to their foliation, they are fractured and brecciated in 
 various degrees, and often exhibit a curious spheroidal or lenticular 
 parting, for which no perfectly satisfactory explanation has been found. 
 
 The monotony of these prevailing aphanitic greenstones is inter- 
 rupted by bands of more coarsely crystalline and less altered rocks, 
 which represent basic dikes of more recent origin. 
 
 THE AFHANITIC GREENSTONES. 
 
 The general character of these widely distributed rocks as seen under 
 the microscope, is shown in PI. X, fig. 2, drawn from a specimen col- 
 lected near the town of Negaunee, where this type is developed even 
 better than near Marquette. In the mass which appears to the 
 unaided eye as quite homogeneous, the microscope discloses long, 
 almost acicular feldspar crystals, embedded in a confused aggregate of 
 hornblende needles, chlorite scales, epidote, quartz, calcite, and cloudy 
 spots, probably derived from leucoxene. The feldspar in these rocks 
 is, as a rule, fresh, and their twinning lamellae are still distinctly visible. 
 Some of the more acicular crystals seem divided at the ends, as is so 
 often the case in semi-vitreous surface rocks whose feldspar microliths 
 are not completely formed. Indeed, in many of their characters, these 
 aphanitic greenstones strongly resemble porphyrites or melaphyres 
 
164 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 whose glassy base has been completely transformed into an aggregate 
 of secondary products. Tneir structure, imperfectly preserved as it is, 
 strongly indicates a superficial origin. 
 
 As typical representatives of these homogeneous pale green rocks 
 may be mentioned : No. 11638, from the mouth of Whetstone Brook, 
 just south of Marquette ; Nos. 11725 and 11726, from the summit of 
 the hill immediately south of the last locality ; No. 11694, collected 
 about an eighth of a mile south of the State road on the line between 
 the southeast and southwest quarters of Sec. 27, T. 48 N., R. 25 W.; and 
 No. 11721, from south of the township road, on the line between Secs. 
 27 and 28, T. 48 N., R. 25 W. 
 
 These aphanitic greenstones appear to have been particularly sensi- 
 tive to dynamic action. We find locally developed in them every de- 
 gree of pressure foliation from a coarse, slickensided breccia to a chlo- 
 ritic slate. The cleavage, however, is developed parallel to a line rather 
 than parallel to a plane, as is the case with a true bedding. There is a 
 tendency to break into rhomboidal prisms or along almost any plane 
 which is parallel to the average direction of dip. 
 
 No. 11696 is a much gashed and brecciated greenstone which adjoins 
 on the north an uralite diabase dike, No. 11695 (see p. 169). It is both 
 schistose and chloritic, but its microscopical structure shows plainly 
 that it was once a diabase, and that its present character is due en- 
 tirely to the action of some great mechanical force. The typical ophitic 
 structure or irregular network of lath-shaped feldspar crystals is still 
 readily discernible. The mechanical action seems to have been rather 
 a stretching than a compression. The feldspar crystals, which are con- 
 siderably altered, are broken and the fragments pulled apart. The 
 secondary chlorite, so common in all stretched rocks (cf. PI. XI, fig. 
 2), is here abundant in the numerous longitudinal cracks, which traverse 
 the rock irrespective of its component minerals. This is always ar- 
 ranged with its scales or fibers perpendicular to the walls of the fissure. 
 
 In addition to such brecciated rocks as the last specimen, very per- 
 fectly schistose varieties of these aphanitic greenstones are common in 
 the southern part of the Marquette area, their strike conforming to that 
 of all the other rocks of this region. These are typically exposed at 
 the mouth of Whetstone Brook (Nos. 11639 to 11643); in the railroad 
 cutting just west of it (No. 11645); on the high hill still farther west- 
 ward (No. 11726); and in the Duluth, South Shore and Atlantic Rail- 
 road cutting just north of the Marquette sandstone quarries (No. 11691). 
 
 For the most part, these rocks are a fine chloritic mass, which, under 
 the microscope, shows a pronounced schistose structure, but only rarely 
 any certain indications of eruptive origin. Very faint but unmistak- 
 able traces of the ophitic structure are nevertheless sometimes visible 
 even in these rocks, as, for instance, in No. 11726, which was entered 
 in the field notes as a “slaty band traversing the massive greenstones 
 above Whetstone Brook.” 
 
Williams. ] LOSSEN’s WORK ON THE GERMAN GREEN SCHISTS. 165 
 
 The history of these schistose greenstones must be deciphered with 
 the conjoint evidence afforded by the microscope and a study of their 
 relations in the field. The occasional survival of the characteristic 
 diabase structure even in some of the more foliated forms, taken in 
 connection with their evident identity with and gradual transition into 
 the massive varieties, appears to be sufficient proof that, with the 
 exception of certain unimportant tuff deposits, these green schists have 
 been derived from basic eruptives through the agency of intense me- 
 chanical and chemical action. 
 
 The closest analogy to the rocks of the southern Marquette green- 
 • stone area is to be found in the metamorphosed diabases of the eastern 
 Hartz. These rocks have been minutely studied and for the first time 
 successfully deciphered by K. A. Lossen, of Berlin. His descriptions 
 could be applied almost verbatim to the Marquette greenstones ; and 
 each of these two similar areas can but have additional light thrown 
 upon its interpretation by the facts afforded by the other . 1 Lossen dis- 
 tinguishes between the coarse grained or granular (kornig) and the 
 fine grained (aphanitisch) diabase, as has been done in the area here 
 under discussion. He finds that both rocks, but especially the apha- 
 nitic type, are very sensitive to dynamic action, and that in the process 
 of mountain making they have been to a large extent passively meta- 
 morphosed and converted into breccias, “Flaser” diabase and green 
 schists. The last named u grime Schiefer ” are of particular interest 
 to us on account of their resemblance to the schistose rocks of the 
 southern Marquette area. In the Hartz they make a conformable mem- 
 ber of the Wieder schists (hercynian) which are of very considerable ex- 
 tent and are always associated with the aphanitic diabase. The minute 
 and careful studies of Lossen have led him to the conclusion that these 
 schists are not in any way sediments nor even diabase tuffs ( u Sehal- 
 steine v ), but molecularly metamorphosed eruptive rocks, of a fine 
 grained diabase type . 2 The more massive rocks are considered to rep- 
 resent old lava flows which occurred while the accompanying sedi- 
 ments were being deposited, and the idea that the green schists of the 
 Wieder horizon were once also massive diabases, is based both upon 
 the field relations of these rocks and more especially upon the frequent 
 remains of the diabase structure which they still contain. 
 
 The published descriptions of many other green schist areas in Eu- 
 rope — notably in Bavaria, Saxony and the Taunus — show that they 
 possess a strong resemblance to those of Michigan and the Eastern 
 Hartz, and it is not improbable that they also may have had a similar 
 origin. 
 
 1 The descriptions of Lossen are contained in the explanations to the special geological map of Prus- 
 sia and Thuringia (Erlauterungen zur geologischen Spocialkarte von Preussen und den tjiiiringischon 
 Staaten) sheets Pansfelde (1882), and Wippra (1883). 
 
 2 " Dio raikroskopische Untersuchung characteristischor Vorkommen dioser typisclion Diabas- 
 aphaniten vergesellschafteten griinen Schiefer hat orgeben, dass sie, wenn niclit insgesammt, doch 
 grossentheils als unter Drackschieferunj' M rnolecular umgeioandelte Diabase aufziifassen sind.” Ibid., 
 Bl. Wippra, p. 27 ; (cf. also p. 46 and Bl. Pansfelde, p. 52). 
 
166 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 A noteworthy feature of the aphanitic greenstones and greenstone 
 schists of the southern Marquette area, and one which is exhibited in 
 a still more marked degree by the similar rocks occurring near the 
 town of Negaunee (see the following section), is their frequent. division 
 into spheroidal, ovoid, lenticular or more irregularly shaped masses. 
 These differ very much in size, as well as form, and often show a tend- 
 ency to fit together like stones in a mosaic, although they are always 
 separated by interlacing bands of a softer, more schistose and gener- 
 ally darker material. These anastomosing bands seem to wind about the 
 harder and more massive cores, becoming thinner or thicker according 
 as the masses approach each other more closely, or are more widely 
 separated by the rounding off of their corners. This peculiar struct- 
 ure, which appears to be only local in its development, may be seen at 
 the mouth of Whetstone Brook in Marquette, near Baldwin’s kilns, near 
 Negaunee (NE J of NW J of Sec. 28 W., T. 48 N., R. 26 W.), and on the 
 south side of the Carp River along the logging road leading northward 
 from the east end of Teal Lake. The accompanying diagram (Fig. 26), 
 drawn from the last named exposure, illustrates the general character 
 of this structure. 
 
 Fig. 26. — Diagram to illustrate spheroidal parting in aphanitic greenstone. Carp Kiver. 
 
 Scale, 3 feet to the inch. 
 
 The cores generally seem to be quite massive, but in some cases they 
 have a latent foliation which is developed by weathering. Where the 
 rock has become decidedly schistose, as was observed in one part of 
 the Carp River exposure, these cores are pulled out into long interlock- 
 ing lenses, which have their longest axes parallel to the foliation. (See 
 Fig. 27, p. 177.) 
 
 Such a structure as that above described appears to be not uncom- 
 mon in the greenstones and greenstone schists of the Northwest. It 
 is well known to the Canadian geologists, who have designated the 
 rocks exhibiting it as “concretionary traps.” It is described by Dr. 
 Andrew ‘C. Lawson, in his report on the Lake of the Woods, in the fol- 
 lowing terms : 
 
 This structure consists of the rock being divided into moreor less irregularly spheri- 
 cal or ovoid masses, varying iu diameter from 2 to 3 inches to as many feet. These 
 ovoid masses are not in close contact, but are separated from one another by an in- 
 
WILLIAMS'. 1 
 
 SPHEROIDAL PARTING IN THE GREENSTONES. 
 
 167 
 
 terstitial material. Tlie concretionary masses are at their points of nearest approx- 
 imation to each other, generally about half an inch or an inch apart, no matter what 
 may be their size, so that when the ovoid masses are large, the interstitial material 
 appears in section as thin, anastomosing sheets, in which is developed a schistosity 
 parallel to the outlines of the ovoid masses they inclose. The interstitial filling is gen- 
 erally of a darker color, more chloritic, softer, and of a finer, more homogeneous texture 
 than the ovoid masses, and weathers out, often leaving the latter, in sect ions afforded 
 by glaciated surfaces, surrounded by sharp little trenches. 
 
 The ovoid masses are uniformly arranged as regards the direction of their long axes, 
 and each one is surrounded by a sharp border half an inch wide, of a dark greenish 
 gray color, which has been more resistant to weathering agencies than the rest of 
 the rock. The ovoid masses present as the result of weathering a rough or pimpled 
 surface of porous aspect and bleached greenish white color. The interstitial filling 
 is firmer in texture and softer than either the ovoid masses or their border, and is 
 intermediate between them in color, with a brownish yellow tinge. 
 
 In the hornblende schists this ovoid structure in the rock takes a somewhat different 
 aspect, and presents the appearance of thin anastomosing sheets of dark green, soft 
 chloritic material, sometimes enveloping completely ovoid or irregularly shaped por- 
 tions of the hornblende schist, and at others losing themselves in a tapering, dis- 
 connected fashion in the main mass of the rock. 1 
 
 It is evident upon the most superficial examination that this struct- 
 ure is in no way “ concretionary , w as that term is commonly under- 
 stood. Nor is it possible to suppose that the harder ovoid masses were 
 originally ejected fragments, which have become imbedded in a finer 
 matrix of volcanic material forming a true agglomerate. A sufficient 
 objection to this hypothesis is the fact that these harder masses so 
 frequently fit together like parts of a mosaic. 
 
 In many instances the spherical or ovoid form of the disjointed 
 fragments is so perfect that the structure strongly resembles the 
 spheroidal parting, developed in a latent form in eruptive rocks by 
 cooling, and made more distinct by weathering. This, which is really 
 a perlitic structure on a large scale, frequently extends through large 
 masses of eruptive material 5 and the descriptions and photographs 
 kindly furnished the writer by Mr. Whitman Cross, who has studied it 
 in Colorado, indicate many points of striking resemblance to the struct- 
 ure of the Lake Superior greenstones. It is quite possible that the 
 phenomenon may in certain cases be due to contraction, although in 
 others the irregular shape of the fragments, as well as their occurrence 
 in fragmental rocks, indicates another origin. 
 
 A structure showing many points of resemblance to that here de- 
 scribed is presented by the well known green schists (griine Schiefer), 
 occurring near Hainichen, in Saxony, and the explanation afforded by 
 the study of their very favorable exposures may assist our understand- 
 ing of the parting in the Lake Superior greenstones. The fragments 
 of the Saxon green schists, in spite of the great difference in their size 
 (varying from that of a pea to that of a house), are so rounded that they 
 were formerly regarded by C. F. Nauruan n as a conglomerate. 2 Never- 
 
 1 Geol. and Nat. History Survey of Canada, Annual Report for 1885 (new series, Vol. 1); Report 
 CC on the Lake of the Woods, by A. C. Lawson, pp. 52, 53. 
 
 2 Erlauterungen zur geogn. Karte des Konigreichs Sachsen, pt. 1, 1834, p. 09. 
 
168 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 I BULL. 62. 
 
 theless tlieir fitting together convinced subsequent observers that the 
 structure must be due to brecciation in situ. 1 These rocks have more 
 recently been carefully studied by A. Rothpletz, who was able to trace 
 the structure downward into a series of interlacing joints, and who ex- 
 plains the rounded character of the fragments and the production of 
 much of the interstitial material by the rubbing together, under the 
 •action of intense orographic pressure, of a mass already finely subdi- 
 vided by cracks. Fig. 4 of Rothpletz’s plate gives a fair representation 
 of some of the Lake Superior occurrences. 2 
 
 The hypothesis of the mechanical origin of this curious parting in the 
 greenstones and greenstone schists seems best to explain the following 
 facts : 
 
 (1) Its occurrence in fragmental rocks. 
 
 (2) The often very irregular shape of the fragments. 
 
 (3) The interlocking of the same into a mosaic. 
 
 (4) The fact, noticed by Lawson, that the thickness of the interstitial 
 layer is independent of the size of the fragments. 
 
 (5) The fact, also noticed by the same observer, that the interstitial 
 layer in horneblende schists often loses itself in the rock without com- 
 pletely surrounding a fragment. 
 
 (6) The identity in petrographical character of all the cores in the 
 same mass. 
 
 (7) The similarity, except where it is more altered, of the interstitial 
 material to that forming the ovoid cores. At the Carp River locality 
 (see p. 176) the cores contain small white feldspar crystals, which are 
 also present in the layers which separate them. 
 
 COARSE GRAINED DIKE ROCKS. 
 
 The fine grained aphanitic greenstones and greenstone schists which 
 prevail over the southern Marquette area are intersected by many bands 
 of coarser material whose eruptive character is still evident in their 
 microscopic structure. These represent later dikes of a basic character 
 which have broken through the older rocks, and which on account of 
 their more recent eruption are less altered. One of the most typical of 
 these is exposed on the small island near the end of the Cleveland ore 
 dock in Marquette. This small island consists of two portions con- 
 nected by a narrow neck. The southern part is composed of a hard, 
 compact, brown rock, which is sometimes quite coarse grained or por- 
 phyritic. Its color and the abundance of epidote which is macroscop- 
 ically visible indicate extensive alteration. Under the microscope a 
 specimen from this locality, No. 11649, is seen at a glance to be a typ- 
 ical diabase. Although every vestige of the original pyroxene has been 
 
 1 Naumann : Erlauterungen der geogn. Karte der Umgegend von Hainichen im Konigr. Sachsen 
 1871, p. 11. Rud. Credner: Das Griinschiefersystem von Hainichen, Zeitschr. fur die gesammten, 
 Naturwiss., vol. 47, p. 127, 1876. 
 
 2 Ueber mechanische Geateinsuanwandlungen bei Hainichen in Sachsen, part 2. Zeitschr. Deutsch. 
 geol. Gesell., vol. 31, pp. 374-397. PI. IX, 1879. 
 
WILLIAMS.] 
 
 DIABASES SOUTH OF THE MARQUETTE. 
 
 169 
 
 replaced by a finely fibrous green hornblende (uralite), yet the char- 
 acteristic ophitic or diabase structure is still perfectly preserved. The 
 lath-shaped feldspar crystals are but slightly altered and the spaces 
 between them are as sharply defined as when the rock first solidified. 
 
 The northern portion of this little island shows the same diabase in a 
 much more altered form. The rock has a pale greenish color, and, though 
 quite massive in the center, is schistose on either side. 
 
 Nos. 11651 and 11652, the former from the massive and the latter from 
 the schistose portion of this rock, offer additional examples of the fact so 
 frequently observed in the Menominee River greenstones, viz, that the 
 feldspar of those rocks which have been subjected to the greatest pres- 
 sure is more broken, but, as a rule, less altered than that in rocks which 
 have experienced less violent mechanical action. Both of these speci- 
 mens show positive evidence in their structure that they were once 
 diabases. In both the ophitic arrangement of the constituent minerals 
 is still distinct, but in the more massive rock the chemical alteration has 
 progressed much further than in the other. Here the lath-shaped feld- 
 spar crystals are preserved in outline by the various secondary prod- 
 ucts which supply their place. Fibrous hornblende and leucoxene are 
 abundant and nowhere, in either the thin section or hand-specimen, is 
 there visible any parallelism of arrangement among the components. 
 In the schistose rock, on the other hand, chlorite has largely replaced 
 the hornblende, but the feldspar is almost unaltered. The long, lath- 
 shaped crystals are broken and faulted — the fragments of a single indi- 
 vidual often being separated a considerable distance — but in spite of 
 this the substance is as fresh and the twinning-lamellae are as sharp as 
 in a recently solidified rock. Few better examples could be found of the 
 evident action of pressure upon a solid rock mass. There has been a 
 crushing and a consequent development of schistose structure which 
 the microscope reveals with great distinctness. Along lines where an 
 actual slipping took place, fibrous hornblende, chlorite, and calcite have 
 been quite abundantly developed. 
 
 No more typical exposure of the greenstones of the southern Mar- 
 quette area can be found than that seen in the high hill which rises 
 between Whetstone Brook, the State road, and the railroad. (D on the 
 map, PI. VII.) The freshest rock obtained from the summit of this hill, 
 No. 11724, is one of the best preserved diabases found anywhere south 
 of the Eureka series. The feldspar is perfectly fresh but is much 
 broken and faulted, as in the specimen (No. 11652) last described. The 
 interstices between the fragments are filled with chlorite. The allo- 
 triomorphic pyroxene is now largely replaced by paramorphic horn- 
 blende, although cores of the original mineral are not infrequent in the 
 center of the hornblende areas. Apatite, ilmenite, and leucoxene are 
 also present. 
 
 Nos. 11646, from the southwest corner of the railroad crossing on Front 
 street, Marquette (see on the map, PI. VII.), and 11695, collected just 
 
170 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bIill. 62 . 
 
 north of the state road (in the center of Sec. 27 T. 48 N., R. 25 W.), are 
 also well defined uralite diabases. In both the structure is still intact 
 and the feldspars are generally well preserved, though the augite is wholly 
 uralitized. One rock of exceptional character (No. 11687) which oc- 
 curs within the limits of the southern Marquette area, must not be 
 passed over without notice. This outcrops in a small exposure at the 
 end of the road leading westward from Marquette to the Eureka 
 shaft, about two miles from the city (see map, PI. VII). It is of a light 
 brownish color, and, in spite of an advanced state of chemical altera- 
 tion, it shows plainly the effects of great pressure. It appears once 
 to have been a gabbro, very similar to that occurring at Sturgeon 
 Falls, on the Menominee River (see p. 67), but now its original compo- 
 nents and structure have both disappeared. Interlacing, lenticular 
 areas produce a decided “microflaser” structure, which, in places, 
 even resembles the fluidal appearance of certain vitrophyres. The min- 
 erals now present are a very pale chlorite filled with sharp epidote or 
 zoisite needles, saussurite, quartz, calcite, ilmenite, leucoxene grains, 
 and winding bands of a clear, brown, isotropic substance which looks like 
 opal. This rock appears much shattered in the field and it is in imme- 
 diate contact with the thin, fissile schists in which the Eureka sbaft is 
 sunk. 
 
 GREENSTONES SOUTH OP THE QUARTZITE. 
 
 Some distince south of the Carp River, in the west half of the NW. 
 ^ Sec. 6, T. 47 N., R. 24 W., below the limestones and quartzite, a few 
 much contorted and altered greenstones appear just on the contact 
 with the granite which incloses the Marquette basin on the south. 
 
 No. 11778 may still be recognized as a diabase, though it now con- 
 tains only saussurite, chlorite, epidote, quartz, and leucoxene. 
 
 Nos. 11774 and 11775 are from the same greenstone band, the former 
 massive, the latter schistose. They do not resemble any other rocks in 
 the Marquette area, but they find their analogues in certain remarkable 
 rocks on the south bank of the Carp River, where this is crossed by the 
 road leading noithward from Teal Lake (see succeeding section, p. 175). 
 Sharply defined crystals of reddish feldspar are imbedded in a bright 
 green mass of chlorite and serpentine. The feldspars, although not 
 pulled apart as in rocks which have been subjected to a stretching, show 
 evidences of the action of enormous pressure. Remnants of hornblende, 
 from which the serpentine was probably derived ; ilmenite, surrounded 
 by leucoxene ; and round grains of bright red iron hydroxide are also 
 present in this rock. In the schistose modification, the constituents are 
 pulled out into parallel bands. The feldspars are lath-shaped and 
 smaller, and, without any loss of sharpness in their outline, they are re- 
 placed by calcite, which is surrounded by an opaque black rim. Cer- 
 tain bands in this rock are much finer grained and present the feldspar 
 and hornblende in a much less altered condition. 
 
 No. 11779, from this same locality, is one of the best specimens any- 
 
171 
 
 williams. 1 APHANITIC GREENSTONES NORTH OF NEGAUNEE. 
 
 where collected to show the effects of rock-stretching. It appears once 
 to have been a granite porphyry, but is now very schistose and is col- 
 ored green by the secondary chlorite. Its ground mass is a felt-like ag- 
 gregateof sericite, quartz, and chlorite with a perfectly parallel arrange- 
 ment of the constituents. The large porphyritic feldspar crystals are 
 much broken and pulled apart, always in the direction of the folia- 
 tion, as shown in PI. XIV, fig. 2. Large calcite individuals are sur- 
 rounded by bright green chlorite, and both of these minerals may rep- 
 resent original biotite or some bisilicate. 
 
 ROCKS OF THE NEGAUNEE AREA. 
 
 As has already been stated at the beginning of the preceding chap- 
 ter, two points were selected for the study of the more western portion 
 of the Marquette greenstone belt. One of these was the mining town 
 of Negaunee, situated at the southeast corner of Teal Lake, about 
 twelve miles west of Lake Superior. The town itself is on the iron- 
 bearing Huronian rocks, south of the greenstone belt, whose south- 
 ern edge skirts the northern shore of Teal Lake. Both east and 
 west of the lake the greenstones are bounded on the south by the 
 narrow ridge of white quartzite, whose termination is Mount Mesnard. 
 
 From this quartzite two sections, three miles apart, were run north- 
 ward to the granite and Huronian rocks, which here divide the green- 
 stones into two separate areas. The more southern of these, which we 
 will designate as the Negaunee area, resembles in its general character 
 the region south of the Eureka series near Marquette; while the region 
 north of the Dead Biver, which will form the subject of the succeeding 
 section, is much more like the northern Marquette area. 
 
 The greenstones occupying the region north of Negaunee do not 
 occur in continuous exposures, but rise out of the plain composed of 
 glacial and later deposits in the form of rounded knobs. Both the 
 longest axis of these knobs and the approximately parallel rows in 
 which they are arranged follow the east and west strike, common to 
 ail the rocks of this region. The greenstones are, for the most part, of 
 the much fissured and brecciated, light green and aphanitic variety, 
 described in the last section. They are also very commonly associated 
 with the same coarser and more crystalline eruptives, probably of a 
 much later age, that we encountered south of Marquette. 
 
 As will be readily seen from an examination of Dr. BomingeFs map 
 the Huronian rocks arbund and south of Negaunee and Ishpeming are 
 also penetrated by numerous greenstones. These, as a rule, resemble 
 the more crystalline and later intrusions of the greenstone belt proper, 
 and they may have been contemporaneous with them. 
 
 APHANITIC GREENSTONES. 
 
 The main mass of the greenstone belt near Negaunee is composed of 
 the fine grained or aphanitic rock which has been described in the last 
 
172 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62 . 
 
 section as characteristic of the region south of Marquette. They be- 
 long to Lossen’s type of “dichte Diabase” and always show more ad- 
 vanced chemical alteration than the coarser rocks. This is to be ex- 
 plained by their finer grain and also from the fact that they are older 
 and have been subjected to more dynamic action than the others. In 
 the field these rocks are found to be much brecciated and not infre- 
 quently quite perfectly foliated. They also exhibit the peculiar spher- 
 oidal parting already described, p. 166. 
 
 The microscopical appearance of a fair average type of these aphanitic 
 greenstones (No. 11747, from Baldwin’s Kilns) is represented in PI. X, 
 fig. 2, but they show considerable variation in both structure and com- 
 position. In none is any trace of pyroxene now to be found, and yet they 
 were probably once typical diabases. Their mineralogical differences are 
 mainly dependent on the relative proportions of hornblende and chlorite. 
 The preponderance of one or another of these minerals may-. be attrib- 
 uted to a more or less advanced stage of chemical alteration, but cer- 
 tain differences in structure have probably always existed. The grain 
 may vary considerably in its coarseness, while the long acicular feld- 
 spar crystals, so abundant in some specimens, are wholly wanting in 
 others. 
 
 No. 1 1736 was collected on the road from Negaunee to Baldwin’s 
 Kilns, just beyond the Carp River, from about the center of the SW 
 J of the NE J of Sec. 29, T. 48 N., R. 26 W. It is comparatively coarse 
 grained and little altered. Under the microscope it appears as a con- 
 fused aggregate of fibrous hornblende, a cloudy, opaque, indetermin- 
 able substance and some original feldspar whose crystals are much 
 broken. 
 
 No. 11744, obtained from an isolated knob of greenstone, situated in 
 the S W J of the NE J of Sec. 28, T. 48 N., R. 26 W., on the longer road 
 to Baldwin’s Kilns, about one mile east of where the last specimen was 
 collected, is much like it in appearance and microscopic character. 
 The only differences are due to the more advanced alteration of the lat- 
 ter rock. Here chlorite is abundant and the feldspar hardly visible. 
 
 No. 11745, from the same road as the last, but much nearer the Kilns, 
 shows the spheroidal parting or brecciatiou in a very perfect manner. 
 The grain is very fine, and the incomplete skeleton-like forms of por- 
 phyritic feldspar crystals are numerous. The mass itself is now largely 
 chloritic, but looks as if it might once have been a finely porphyritic 
 rock. 
 
 No. 11747, found at the same locality, is the one from which PI. X, 
 fig. 2, was drawn. It is similar in structure to the last specimen, but 
 its grain is coarser, and fibrous hornblende is still abundant in. its 
 groundmass. The porphyritic feldspar crystals are broken, faulted 
 and separated. 
 
 No. 11748 is a schistose modification of 11747. This rock has a much 
 finer grain than the other, but no evidence of schistose, structure is ap- 
 
WILLIAMS. | 
 
 COARSE GRAINED GREENSTONES. 
 
 173 
 
 parent under the microscope. The chemical alteration has progressed 
 so far that hardly any of the substances remaining have much action 
 on polarized light ; nevertheless, faint traces of small acicular feldspar 
 crystals are visible. 
 
 One massive greenstone, No. 11740, found just north of Baldwin’s 
 Kilns, in the NW J of Sec. 21, T. 48 N., R. 26 W., is striking on 
 account of its being mottled with round white spots from 5 mm to 6 mm 
 in diameter. The rock is somewhat darker than usual in a rim around 
 these spots, and the whole effect is exactly that of a variolite. Under 
 the microscope the rock itself is found to be composed almost wholly 
 of green fibrous hornblende, together with some opaque grains and 
 saussurite. The round whitish spots are very largely composed of 
 saussurite or a very fine mosaic, in which sharply defined hornblende 
 crystals are imbedded. They do not show the least trace of a radial 
 or sheaf-like arrangement, such as is characteristic of a true variolite. 
 These spots are not unlike those found in the banded greenstones of 
 the Brook section (see p. 157) in their composition and structure, but 
 they are very much more regular and uniform in their shape. 
 
 Other specimens of these aphanitic greenstones, as for instance Nos. 
 11793, 11795, 11796, and 11797, collected along the line of the old 
 logging road, which leads from the eastern end of Teal Lake north- 
 ward to Johnson’s Camp, in the SE £ of Sec. 13, T. 48 N., R. 27 W., are 
 quite like those above described from the neighborhood of Baldwin’s 
 Kilns. 
 
 COARSELY CRYSTALLINE GREENSTONES. 
 
 No. 11749, collected in the extreme northeast corner of Sec. 21 T. 
 48 N., R. 26 W., northeast of Baldwin’s Kilns, is an unusually beauti- 
 ful rock. The structure is coarse grained and rather granular, in 
 spite of the feldspar crystals being idiomorphic. The large individuals 
 of hornblende also, to some extent, have their characteristic crystal 
 form. They are frequently changed to chlorite or to fibrous horn- 
 blende, but still oftener, although bleached to a pale green color, they 
 retain their compact texture and show a twinning structure. There 
 are no present indications that this rock ever contained pyroxene, and 
 it is therefore to be designated as a diorite. The hornblende shows, 
 in the process of its- alteration, a curious tendency to concentrate the 
 deep green color around the periphery of the crystals ; also the fraying 
 out of their edges into hornblende needles similar to those described 
 by Becke and Van Hise as secondary growths, produced by regularly 
 orientated accretions of hornblende substance. All of these features 
 are shown in Plate XII, fig. 1, which represents the microscopic ap- 
 pearance of this rock. The feldspar is filled with epidote or actinolite 
 • needles. Large areas of bright green chlorite also occur which contain 
 sometimes sharp epidote crystals, but more commonly fibrous horn- 
 blende. Leucoxene after ihnenite is abundant. 
 
174 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. GB. 
 
 No. 11739, from the southeasterly portion of the SW ^ of the NW J 
 Sec. 21, T. 48 N., E. 2(3 W., just north of Baldwins Kilns, is a dioritic 
 rock much like the last, but it is considerably more altered. The horn- 
 blende is more fibrous, the feldspar more saussuritized, while the 
 original structure is also beginning to suffer. 
 
 No. 11746 was taken from a well marked dike which intersects the 
 spheroidally parted, aphanitic greenstones, near Baldwin’s Kilns. Here 
 the diabase or ophitic structure is perfectly developed, and there is 
 no reason to doubt that the pale green, fibrous hornblende, which now 
 fills the allotriomorphic spaces between the lath-shaped feldspar crys- 
 tals is secondary after augite. The most interesting feature of this 
 rock is its amygdaloidal structure which was observed in no other Mar- 
 quette greenstone. Several small amygdules are filled with brightly 
 polarizing epidote, while one large circular cavity, measuring four 
 millimeters in diameter, has its sides coated with radiating epidote 
 needles and its center filled with calcite. 
 
 No. 11741 is the rock exposed at Baldwin’s Kilns. It is much jointed 
 but quite massive. Under the microscope it appears like the specimen 
 last described, except that it is finer grained and devoid of amyg- 
 daloidal cavities. The structure of this rock is perfectly preserved. 
 It was once a typical diabase, although now no trace of pyroxene 
 remains. 
 
 Another of the more coarsely crystalline dike rocks of the Negaunee 
 greenstone belt was obtained near the granite contact in Sec. 13, T. 48 
 N., E. 27 W., two and one-half miles north of Teal Lake. This (No. 
 11791) is a typical uralite diabase, as is shown both by the distinct 
 traces of ophitic structure and by the frequent cores of pale reddish 
 brown augite which still remain in the fibrous hornblende. Ilmenite, 
 partially changed to leucoxene, is also present in forms especially char- 
 acteristic of diabase. The original structure has been considerably 
 obscured by chemical changes. The feldspar is partly recrystallized to 
 a mosaic, and epidote, chlorite, and quartz have been secondarily de- 
 veloped. 
 
 As has been above remarked (p. 171), the greenstones which occur so 
 abundantly in the iron bearing Huronian rocks both north and south of 
 Negaunee are apparently identical with the coarse grained, younger 
 rocks of the greenstone belt proper. Still they show the effects of hav- 
 ing been subjected to enormous pressure which has frequently produced 
 in them a schistose structure ; and as this is, in every case, conformable 
 to the general strike of all the rocks of this region, we must conclude 
 that these greenstones were intruded before the folding of the Huronian 
 sediments was completed. 1 
 
 Specimens were collected from the prominent exposures of these 
 greenstones near the town of Negaunee. They are ail rather coarse 
 uralite diabases of the type last described from the greenstone belt. 
 
 See sections by Brooks, Atlas to Geol. Survey Michigan, Pis. in and v. 
 
WILLIAMS.] 
 
 CARP RIVER TUFFS. 
 
 175 
 
 No. 11754, collected from the SW J of the SW J Sec. 6, T. 47 N., R. 26 
 W., near the mouth of the Jackson mine, has a well preserved diabase 
 structure. Its pyroxene is wholly changed to pale secondary horn- 
 blende ; its feldspar is filled with epidote, while chlorite and leucoxene 
 are common. 
 
 No. 11755, from a high hill somewhat farther east, is essentially the 
 same rock. It contains epidote and chlorite even more abundantly. 
 
 No. 11756 was collected from a small greenstone knob just east of 
 the hotel (Breitung House) in Negaunee. This rock has been quarried 
 and may be plainly seen to have been rendered partially schistose by 
 pressure. Under the microscope it is like the preceding rocks except 
 that alteration has here progressed further — so much so as to have 
 obscured, though it has not obliterated, the original diabase structure. 
 Chlorite, epidote, and calcite are among the prominent constituents. 
 
 Nos. 11758 and 11759 are from the greenstone bluffs which skirt the 
 southern shore of Teal Lake near its eastern end. The former is the most 
 massive, the latter a schistose variety of this exposure. The massive rock 
 is a uralite diabase of the ordinary type, retaining its original structure 
 and also occasional cores of red augite in the masses of secondary horn- 
 blende. Besides the usual chlorite, epidote, and leucoxene, there is con- 
 siderable quartz present in this rock. The second specimen, taken from 
 the schistose band on the south side of this greenstone ridge, shows 
 evidence of intense mechanical and chemical action. The original 
 structure has almost wholly disappeared, while its component minerals 
 are calcite and chlorite, together with a little quartz and leucoxene. 
 Rarely these secondary products have preserved the outline of lath- 
 shaped feldspars, which show that they have been much broken and 
 pulled apart by the stretching action to which the rock has been sub- 
 jected. 
 
 THE STRETCHED FRAGMENTAL ROCKS ON THE CARP RIVER. 
 
 An enigmatical group of rocks was met with near the center of the 
 Negaunee greenstone belt, where the old road leading to Johnson’s 
 logging camp crosses the Carp River. This locality is in the NE £ 
 Sec. 25, T. 48 N., R. 27 W. The first rock south of the river is exposed 
 in a low wall which rises just west of the trail. (No. 11798.) This is 
 apparently a dark colored, schistose greenstone, standing nearly vertical 
 and filled with red granite fragments of all shapes and sizes, though 
 generally with well rounded outlines. The dark green matrix also con- 
 tains much of the red material in a finely divided form, often resembling 
 sharp crystals. The rock itself is much brecciated and cut by cross- 
 gashes, as if it had been subjected to a stretching tension. 
 
 Under the microscope the dark green portion of this rock is found to 
 consist entirely of chlorite, the scales of which are arranged parallel to 
 each other and to the cleavage planes of the mass. Its color, when free 
 from inclusions, is a clear, bright green, but it frequently contains con- 
 
176 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 siderable black or brownish opaque material, which is arranged in long, 
 sinuous lines following the foliation. The reddish inclusions are almost 
 altogether orthoclase, colored by a fine, unevenly distributed, globu- 
 litic dust. A striated feldspar may also be occasionally observed. The 
 orthoclase is partly in sharply defined crystals, but more commonly in 
 irregular and angular fragments. These range through all sizes down 
 to the most microscopic dimensions. The smallest bits are locally 
 scattered so thickly through the chlorite as to give the rock a decid- 
 edly clastic appearance. 
 
 The chlorite matrix is of that peculiar character which we have 
 already had occasion to notice as characteristic of stretched greenstone, 
 particularly in the Menominee Valley (see pp. 82, 83, and PI. XI, 
 fig. 2). This chlorite must have crystallized after the orthoclase frag- 
 ments had come into their present relative positions, as may be seen 
 from the relations of its scales to the feldspar, and also by the bending 
 around these fragments of the sinuous bands of opaque matter which 
 the chlorite sometimes contains. We may go even further and assert 
 that the chlorite could not have been formed prior to the stretching 
 action. Proof of this is to be found in the fact that some of the ortho- 
 clase inclusions may be plainly Seen to have been broken during this 
 process and their fragments to have been separated but a short dis- 
 tance and always in the direction of the foliation ; and yet the same 
 chlorite which forms ths whole matrix fills these late fissures. 
 
 It is impossible to state auything positive with reference to the origin 
 of this chlorite ; and still its universal presence in the stretched green- 
 stones would indicate that this particular form of dynamic action upon 
 a mass of the proper chemical composition is, in some way, neces- 
 sary, or at least very favorable to its production. 
 
 No. 11799, from the same locality, is essentially like the last speci- 
 men, except that the included feldspar is lighter colored and perhaps 
 more altered to kaolin or muscovite. The matrix is not so purely 
 chloritic, but contains much finely divided feldspar. The stretching 
 action is here even more apparent, a single feldspar crystal being pulled 
 out to over double its original length and its fissures being filled with 
 the same green chlorite. 
 
 If we trace this ridge farther south it develops into a finer grained 
 and more schistose greenstone, which is free from the larger granitic 
 inclusions but is mottled with small white spots (No. 11800). These are 
 found upon closer examination to be feldspar crystals. Under the 
 microscope this rock is quite like those above described, but it shows 
 much more distinctly the effects of dynamic action. The grain is very 
 uneven. In some places the feldspar crystals are thickly crowded and 
 are cemented by the usual chlorite in which epidote is abundant; in 
 other places the matrix is a very fine grained aggregate of chlorite, 
 sericite, quartz, and feldspar, containing considerable opaque substance 
 and possessing a micro-flaser structure produced by the winding of its 
 
williams.] EFFECT OF STRETCHING ON SPHEROIDAL PARTING. 177 
 
 parallel bands about the occasional feldspar inclusions. These latter 
 are much pulled out in the direction of the foliation and have their 
 interstices filled, sometimes by the chlorite, but oftener still by calcite. 
 
 No. 11801 is a more weathered specimen of this same rock, which 
 shows with great distinctness the spheroidal parting described above 
 (see p. 166). The stretching action is here displayed by the pulling 
 out of the spheroids into a system of interlocking lenses, as represented 
 in Fig. 27. Under the microscope this rock shows the effect of the me- 
 
 Fig. 27 — spheroidal parting of aphanitic greenstone pro- 
 duced by brecciations; drawn out into lenses by pres- 
 sure. Scale same as in Fig. 26. 
 
 chanical action in the extremest degree. The matrix is very schistose 
 and consists of a gray, indeterminable, almost isotropic mass in which 
 minute flakes of sericite are distinguishable. The feldspar crystals 
 are so altered that they seem to grade imperceptibly into the matrix, 
 leaving their original shapes but indistinctly outlined. The dark green 
 chlorite occurs only in rare patches. 
 
 No. 11802 is from the interstitial mass between these lenses. It is a 
 finely fibrous, felt-like, sericitic mass, in which the scales are so strictly 
 parallel that the entire slide extinguishes the light between crossed 
 Nicol prisms almost like a homogeneous crystal. There are besides pres- 
 ent only small patches of a light brown, isotropic substance, some little 
 quartz in isolated areas, and long stringers of leucoxene, out of which 
 minute but sharp, highly refractive octahedrons have been developed 
 (anatase ? cf. No. 11130, p. 131). 
 
 No. 11803, also from this interstitial material, contains white feldspar 
 crystals like the more massive cores. A microscopic examination shows 
 that this specimen is in all respects identical with the rock which it sur- 
 rounds. The schistose structure is due to a crushing accompanied by 
 a tension in one direction. The effect of this is so striking on the in- 
 cluded feldspar crystals that it has been selected for illustration. (PI. 
 XIV, fig. 2.) 
 
 After a careful study of this suite of rocks, which is distributed over 
 a considerable area, it is impossible to escape the conviction that 
 they are of a fragmental character. Neither their structure nor their 
 
 Bull. 02 12 
 
178 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 mineral composition resembles that of any known eruptive rock while 
 the sudden variations in grain, the irregular and angular shape of the 
 feldspar inclusions, and, above all, the extreme differences in the size of 
 even such of these inclusions as lie side by side can be reconciled only 
 with a clastic origin. Still these rocks do not bear the stamp of true sed- 
 iments, and the most probable hypothesis of their nature which the 
 writer can offer is that they are deposits of volcanic ejectamenta which 
 have subsequently been rendered schistose by dynamic agencies. The 
 irregular and angular fragments of red granite must be regarded as 
 material broken from off' the underlying rock masses and hurled out by 
 the violent explosive force, along with much finer rapilli, sand, and 
 ashes. These rocks seem to agree very closely with the agglomerates 
 described by Mr. A. O. Lawson, of the Oanadiau Geological Survey, as 
 attaining an extensive development in the Lake of the Woods region. 
 These are filled with angular fragments and have also been subjected 
 to great pressure. Mr. Lawson’s opinion regarding the origin of these 
 agglomerates is the same as that above advanced. 1 
 
 The presence, as here, of the spheroidal or lenticular parting in rock 
 of fragmental origin is sufficient to show that it must be a mechanical 
 and not a molecular phenomenon. 
 
 ACID ROCKS. 
 
 There were no acid intrusives encountered within the Negaunee green- 
 stone area proper, nor do the granites which skirt the northern edge of 
 this belt present any points worthy of especial note. 
 
 No. 11790 is the granite in immediate contact with the greenstones at 
 the end of the section which was run northward from Teal Lake. It 
 was found at the Johnson logging camp in Sec. 13, T. 48 N., B. 27 W. 
 This is a typical granitite in which quartz is not very abundant. The 
 biotite is quite altered and bleached. The feldspar is particularly dis- 
 tinguished by its beautiful zonal structure, which the incipient kaoliniza- 
 tion has brought out all the more distinctly. This feldspar shows the 
 effects of pressure, and in one instance this can be plainly seen to have 
 resulted in the production of a microcline structure. One small, sharp _ 
 crystal supposed to be orthite was observed in this rock. Apatite and . * 
 zircon also occur, and occasionally a few rutile needles are secondarily 
 developed in the altered mica. 
 
 No. 11738 is from the granite in contact with the greenstone just $ 
 north of Baldwin’s Kilns. This rock is completely crushed, the constit- j 
 uents being in some cases so pulverized as to give the specimen, when 
 seen under the microscope, almost the appearance of a fragmental de- j 
 posit. The mica is here much altered, and among secondary products 
 has given rise to an abundance of most delicate rutile needles, which 
 often form the characteristic twins. 
 
 Geol. and Nat. Hist. Survey of Canada. Ann. Rept. for 1885, p. 49, CC, 
 
WILLIAMS.] 
 
 QUARTZITE NOVACULITES. 
 
 179 
 
 Here may conveniently be recorded some observations made on the 
 quartzite of the ridge which borders the greenstones on the south in the 
 neighborhood of Negaunee. This quartzite mass is composed on its 
 northern or lower side of compact, even grained, thinly laminated 
 rocks, varying in color from black to the lighter shades of green, yellow, 
 and drab. At one point, near the northeast corner of Teal Lake, these 
 have been quite extensively quarried as novaculites, although they are 
 of a different character from the novaculites occurring near Marquette. 
 These rocks have the usual east and west strike and dip steeply to the 
 south. These so-called novaculites are again underlaid by conformable 
 beds of a coarse, white quartzite conglomerate, which in its turn is in 
 immediate contact with the greenstones. The best locality for seeing 
 these contacts is on the wood road leading northeastward from the 
 slaughter-house on Teal Lake. (NVY J Sec. 31, T. 48 N., E. 26 W.) 
 
 No 11785 is a nearly black specimen of the novaculite. Under the 
 microscope the fragmental character of this rock is at once apparent. 
 It is composed of irregular quartz and altered feldspar grains in nearly 
 equal proportions. In the finer cement biotite has abundantly crystal- 
 ized. An occasional zircon crystal would seem to indicate that the rock 
 is the stratified debris of an old granite. The present foliation of these 
 novaculites is to be regarded as a slaty cleavage due to pressure, rather 
 than an original stratification. 
 
 The conglomerate between the novaculite and greenstone, and form- 
 ing the base of the Huronian quartzite, is composed of large grains 
 and pebbles of granitic quartz, imbedded in a fine, silky matrix of 
 sericite. (Nos. 11787 and 11788.) 
 
 ROCKS OF THE NORTHERN AREA. 
 
 The second point selected for the examination of the western portion 
 of the Marquette greenstone belt is near the center of Sec. 9, T. 48 
 N., E. 2G W. Here a camp was established and from it were studied 
 the greenstones represented upon Dr. Eominger’s map as occurring 
 north of the Dead Eiver. The rocks within this area present a much 
 more varied character than those of any of the other areas examined. 
 Indeed, although a considerable collection of specimens was made, it is 
 not for a moment supposed that all the types of massive rocks which 
 occur in this region were obtained. Enough, however, will be noticed 
 to indicate the general character of the area and at the same time to 
 illustrate the extreme variety offered by different, and often nearly 
 contiguous, outcrops. 
 
 In its chief features, this area more closely resembles the northern 
 portion of the belt near Marquette, just as the southern branch near 
 Negauuee, as stated in the preceding section, is more like the south- 
 ern Marquette area. Still, the more recent eruptive rooks which pene- 
 trate the banded green schists far exceed, both in amount and variety, 
 those to be found nearer Marquette. 
 
180 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62 . 
 
 UNALTERED BASIC INTRUSIVES. 
 
 At the falls of the Dead River, in the southwest corner of Section 9, 
 the “ arenaceous slate group” of Rominger is well exposed. This con* 
 sists here of thinly bedded slates which strike N. 75° W. and stand 
 nearly vertical, with perhaps an inclination to the south. The upper 
 part of the fall is a steep incline over the slates, but the lower portiou 
 is a clear fall of from twenty-five to thirty feet, occasioned by several 
 trap dikes which run nearly east and west. These are coarse grained, 
 fresh, and sometimes porphyritic. 
 
 No. 11814, from one of these dikes, is found, under the microscope, to 
 be a very fresh and typical olivine diabase, quite like that of the great 
 dike on Lighthouse Point, Marquette. The structure is typically 
 ophitic. The porphyritic appearance is occasioned, not by single indi- 
 viduals of feldspar, but by concretionary aggregates of this mineral. 
 The olivine, which frequently presents crystal outlines of great sharp- 
 ness, is sometimes completely, sometimes only slightly serpentinized. 
 
 No. 11826 was collected from an outcrop beside the road at the south- 
 west corner of Sec. 10, T. 48 N., R. 26 W. It has every appearance of 
 being in place, but the character of the rock, unknown elsewhere in this 
 region, renders it much more probable that it is a portion of a huge glacial 
 erratic which is nearly buried in the drift. Still, the petrographical in- 
 terest of this rock makes it worthy of a description. A close examina- 
 tion shows it to be an olivine gabbro, perfectly fresh and peculiar on 
 account of the abundance and beauty of its olivine. This constituent 
 makes up a large percentage of the entire mass. It is present in ex- 
 tremely sharp and well formed crystals from 0.1 to l mra in diameter. 
 These show the usual hexagonal cross-sections, due to the presence of 
 faces of the prismatic zone and domes. 1 No signs of even incipient 
 alteration are visible in this olivine. The augite and triclinic feldspar 
 are both allotriomorphic, and form much larger individuals than the 
 idiomorpliic olivine which they inclose. Magnetite is abundant in 
 sharp octahedral crystals, showing quadratic sections ; while other ir- 
 regular areas of an opaque black iron mineral may be ilmenite. These 
 latter are often partially bordered by a dark brown mica. No other 
 rock exactly like this is known to me, but in its general character it is 
 allied to the olivine gabbros which play such an important role on the 
 north shore of Lake Superior. 2 
 
 ALTERED COARSE GRAINED ROCKS. 
 
 The coarser grained intrusive rocks, which penetrate the prevailing 
 green schists of the northern area, have, as a rule, undergone a consid- 
 erable amount of chemical alteration. This has more or less completely 
 replaced the original minerals by secondary products ; while, in some 
 
 1 These crystals show indications of twinning, as described by Kalkowsky (Zeitsclir. Kryst. n. Min- 
 eral, vol. 10, ]). 17) but these are not as distinct as the sharpness of the crystals would lead us to expect. 
 2 Of. Irving; Mon. U. S. Geol. Survey, vol. 5. 
 
WILLIAMS. J 
 
 DIORITES OF THE NORTHERN AREA. 
 
 181 
 
 cases, it has also obliterated the original structure. Among these 
 younger eruptive greenstones the same two types can be distinguished 
 as in the Marquette area, viz, diorite and diabase. 
 
 Diorite — Nos. 11828 and 11829 are from an exposure thirty paces in 
 width, on the line between Secs. 5 and 8, T. 48 N., R. 26 W. This rock 
 is sometimes parted into parallel plates so as almost to resemble a slate. 
 In the hand-specimen it is seen to be composed of rather large, well- 
 formed hornblende crystals, which are often hollow at the center, and 
 a reddish feldspar. The microscope shows that the two specimens are 
 identical. The hornblende is idiomorphic, though without terminal 
 planes; the feldspar, on the other hand, is wholly allotriomorpkic. 
 This latter mineral is almost free from twining striations, so that the 
 rock were perhaps more properly termed a syenite. The hornblende 
 preserves much of its compact structure and brownish color. It is 
 frequently changed at the center to a mass of fibrous needles, or even 
 to chlorite, while the exterior remains compact and unaltered. Apatite 
 is very abundant; sphene and magnetite are not uncommon. 
 
 No. 11817, from a wide dike at the northwest corner-post of Section 
 9, of the same township, is of the same type as the last specimens, but 
 more altered. Macroscopically tufts of hornblende crystals may be 
 seen imbedded in a white feldspar substance. Under the microscope 
 this feldspar appears to be mostly altered to a brownish saussurite, in 
 spite of which, however, traces of a stout lath-shape are discernible. 
 The hornblende is much altered to a fibrous form. It frequently has 
 the emerald green color of actinolite, especially around the outer edge, 
 where it is always darker and more compact than at the center. lime- 
 nite, accompanied by leucoxene, is abundant in the rock, though absent 
 in the two last mentioned specimens. It will be noticed that this rock 
 approaches much more nearly than the others to the diabase type, and 
 yet there is no reason to believe that the hornblende is paramorphic 
 after pyroxene. Although it is not compact, it still retains its twinning 
 structure as one of its most common features. 
 
 A still more striking example of idiomorphic, lath-shaped feldspar 
 in a diorite (a structure which Bosenbuscli mentions as not at all un- 
 common in rocks of this class 1 ), is to be found in No. 11831. This was 
 obtained on the line between sections 5 and 8, just east of Nos. 11828, 
 11829, above described. It is entered in the field-notes as a coarse 
 reddish diorite or syenite, having long, green hornblende crystals im- 
 bedded in a red feldspar. On account of its unstriated feldspar, this 
 rock may perhaps be even more properly designated as an amphibole 
 granite, although its structure is in many respects jieculiar. (See PI. 
 XVI, fig. 2.) The feldspar is present in two distinct generations. 
 The earliest of these yielded stoutly lath-shaped crystals, which are 
 wholly idiomorphic. These are mostly unstriated, but have a zonal 
 structure. They are internally changed to a grayish mass, which a 
 
 1 Mikros. Physio#., 2d ed., vol. 2, p. 121. 
 
182 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [ HULL. 62. 
 
 high magnifying power shows to be muscovite or kaolin, while their 
 periphery is composed of clear and fresh feldspar substance. Between 
 these feldspar crystals is a granular aggregate of quartz and a younger 
 feldspar. This latter mineral is also unstriated (though sometimes 
 possessed of the gridiron microcline structure) and much fresher than 
 the older feldspar. With the quartz it frequently forms beautiful 
 micropegmatitic growths. 
 
 Hornblende was most probably the original bisilicate constituent of 
 this rock, but it has undergone an unusual alteration, i. e., the altera- 
 tion to mica. This mineral can be seen under the microscope in brown 
 areas of irregular shape, which have evidently been produced at the 
 expense of the hornblende. 1 They are unevenly colored, being a 
 darker brown in some places than in others. In some cases the new 
 mica crystallizes in sharply defined hexagonal plates. Certain of these, 
 which on optical examination prove to be basal sections, show cleav- 
 age lines parallel to the prismatic faces. These are the so-called 
 pressure figures (“Drucklinien” of the German mineralogists), which 
 are rarely visible in microscopical sections and are strongly indicative 
 of pressure. 
 
 This secondary mica to a considerable extent has turned green by a 
 reduction of its iron to a ferrous state. More rarely the alteration has 
 progressed still further, resulting in complete bleaching, or even the 
 production of chlorite. Apatite is very abundant in this rock; sphene 
 is also common, but its crystals always surround ilmenite grains in 
 such a manner as to suggest that the titanite has resulted from its 
 alteration (see PI. XVI, fig. 2). Chlorite also frequently surrounds 
 the opaque iron mineral. 
 
 Of all the remarkable features which this rock presents, perhaps 
 none is more striking than its hypidiomorphic structure and the 
 presence of the feldspar in two distinct generations without the pro- 
 duction thereby of a porphyritic structure. This is all the more note- 
 worthy in a rock which from its mineralogical composition is to be 
 strictly classed among the granites. 
 
 Xo. 11832, which occurs with the specimen last described, appears 
 to the unaided eye as a compact, fine grained mass through which 
 large glistening hornblende crystals are unevenly distributed. Under 
 the microscope the groundmass of this rock is seen to be composed of 
 lath-shaped feldspar crystals, which are altered sometimes to epidote, 
 sometimes to sericite; allotriomorphic hornblende, frequently changed 
 to chlorite; a little quartz and magnetite in grains and crystals. 
 The sharp quadratic and hexagonal sections are sufficient to iden- 
 tify this species; but we must assume that it is a titaniferous 
 magnetite on account of the very narrow leucoxene border which 
 
 ^osenbusch mentions only parallel growths of hornblende and biotite. The present instance can 
 hardly bo so interpreted, while there is nothing surprising in an alteration which has been so fre- 
 quently observed. (Cf. J. Roth: Allgemeine und chemische Geologie, vol. 1, p. 333, 1879.) 
 
WILLIAMS.] 
 
 DIABASES OF THE NORTHERN AREA. 
 
 183 
 
 frequently surrounds it. The porphyritic hornblende of this rock is 
 sometimes regular, sometimes irregular in outline. It is a later crys- 
 tallization than the groundmass, because it is always filled with the 
 lath-shaped feldspars. This produces the structure which I have 
 recently termed “poicilitic,” 1 and which is characteristic of younger 
 porphyritic crystals, especially hornblende and pyroxene. 
 
 No. 11834, from a ledge 640 steps north and 20 steps west of the south- 
 west corner of Sec. 4, T. 48 N., K. 26 W., is composed of stout, lath-shaped 
 feldspar crystals and large individuals of fibrous hornblende. The for- 
 mer mineral suggests by its form that the rock was once a diabase; the 
 hornblende, however, is not allotriomorphic, but is present in long, col- 
 umnar crystals, which are generally twinned. One of these crystals is 
 bent in the most unaccountable manner. It forms three-quarters of a 
 circle (see Fig. 28), but no satisfactory explanation can be offered for 
 this unusual shape. 
 
 On the whole, this rock is consid- 
 erably altered. Epidote and horn- 
 blende needles are developed in its 
 feldspar, while secondary quartz is 
 quite abundant. In spite of the 
 fibrous character of its hornblende, 
 the structure of this rock is much 
 more suggestive of a diorite than of 
 a diabase. 
 
 Diabase . — Among the altered in- 
 trusive rocks, those which represent 
 the diabase type are all uralite dia- 
 bases. In none was any trace of the 
 original augite observed. 
 
 In No. 11827, from 485 steps west of the southeast corner of Section 
 5, the structure is best preserved. Here the fibrous and in part bright 
 emerald green hornblende retains exactly the allotriomorphic form of 
 the diabase augite. The feldspar is largely altered to a brown, opaque 
 saussurite, and leucoxene has replaced the ilmenite. 
 
 No. 11337, from 815 steps north of the southwest corner of Section 
 4; No. 11848, from 500 steps west of the southeast corner of Sec. 10, 
 T. 48 N., K. 26 W., are both much more altered than the specimen last 
 mentioned. The ophitic structure is best preserved in the latter, 
 although epidote is abundantly developed, while it is altogether want- 
 ing in the former. 
 
 Other of these uralite diabases are finer grained. 
 
 No, 1 1825, from a somewhat schistose greenstone ridge, exposed near 
 the center of the southwest quarter of Section 10, admirably exhibits 
 the effects of crushing. The lath-shaped plagioclase crystals are still 
 
 Fig. 28.— Bent hornblende crystal. Green- 
 stone No. 11834. Magnified 30 diameters. 
 
 1 Am. Jour. Sci., 3d series, vol. 31, 1886, p. 30. 
 
184 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 wonderfully fresh, but are broken, faulted, and pulled apart, while their 
 interstices are filled with the secondary chlorite usual in stretched 
 rocks. There is a delicate granophyre or micropegmatite structure in 
 this specimen — undoubtedly an original feature, as in No. 11675 (see 
 p. 140). The pyroxene is wholly changed to a pale green, fibrous horn, 
 blende, which, to a considerable degree, produces the foliation. Large 
 areas of brown leucoxene, of the variety most characteristic of altered 
 diabase, are also drawn out in the direction of the schistose structure. 
 In one instance this has altered to a network of dark rutile needles 
 imbedded in a yellowish micaceous mineral, as described in No. 11070 
 (see p. 99, and Plate XIII, fig. 2). 
 
 No. 11830, from 700 hundred steps west of the southeast corner of 
 section 5, is a very typical uralite diabase. The structure is still well 
 preserved by the feldspars, in spite of needles of the fibrous hornblende 
 having freely wandered into them. Traces of augite cores remain in 
 this rock. 
 
 No. 11835 is a schistose rock from 640 steps north and 20 west of the 
 southeast corner of Section 5. It has been much altered, and now con- 
 sists mainly of a fine aggregate of fibrous hornblende, feldspar, quartz 
 and calcite. In this lie large porphyritic crystals of hornblende which 
 are wholly altered, especially in their interior. 
 
 BANDED GREENSTONES. 
 
 Striped and banded greenstone schists, like those of Lighthouse Point, 
 Marquette, are very abundant in the northern area. 
 
 No. 11856, from an exposure near the northeast corner of Section 9, is 
 macroscopically identical with the Marquette rocks. Under the micro- 
 scope it would be designated as a hornblende schist. It consists of mi- 
 nute crystalloids of compact green hornblende, together with feldspar 
 which is mostly changed to sericite. Zoisite in crystalloids, like those 
 represented in Fig. 2, p. 27, and about the size of the hornblende, is 
 also present. The structure of this rock is schistose, caused by the 
 parallel arrangement of all the constituents. 
 
 Other banded greenstones from this region, like No. 11818, from near 
 the southeast corner of Section 5 $ 11821, 850 steps north of the south- 
 west corner of Section 4; 11839, 170 steps south of west quarter post of 
 section 4, and 11841, 180 steps north of the same quarter post, are 
 essentially like the specimen just described — mostly a mass of con- 
 fused hornblende fibers with more or less feldspathic substance, quartz, 
 and chlorite. The relative proportions of these components condition 
 their different colors and cause the parallel striping. 
 
 These rocks are so similar to those occurring immediately north of 
 Marquette, that we must apply to them the conclusion already ex- 
 pressed (p. 158) in regard to the origin of these green schists, and regard 
 them as basic tuff deposits, which were contemporaneous with surface 
 flows of diabase and subsequently profoundly metamorphosed. 
 
williams.] FIELD RELATIONS OF THE DEER LAKE ROCKS. 185 
 
 GREEN SCHISTS AND AGGLOMERATES OF DEER LAKE. 
 
 After the work on this paper was practically completed, my atten- 
 tion was called by Prof. Irving to a group of greenstone schists and 
 conglomeratic rocks which lie in the western extension of the southern 
 branch of Ihe Marquette greenstone-schist belt. I was unable to study 
 and collect these rocks in the field, but Prof. Irving furnished me 
 with notes regarding their distribution and mode of occurrence, together 
 with a suite of hand-specimens and thin sections for laboratory study. 
 I incorporate the results of such a study in this place the more will- 
 ingly because the occurrence of these rocks does not in the least differ 
 from that of others closely allied to them, which I carefully exam- 
 ined in the neighborhood of Negaunee. Tbe distinct evidence, more- 
 over, which these rocks afford as to their mode of origin is of great 
 value in confirming the conclusions already reached in regard to cer- 
 tain other analogous, though less distinctly characterized, occurrences. 
 
 These peculiar rocks are best exposed on the south side of Deer Lake 
 in Secs. 33 and 34, T. 48 2L, R. 27 W., Michigan, but they may also be 
 advantageously seen farther to the northwest, in Secs. 20, 21, 29, and 30 
 of the same township. 
 
 The following field-notes were furnished me by Prof. Irving : 
 
 On the road going northward from Ishpeming to Deer Lake furnace a belt of 
 quartzite dipping southward is crossed in the middle of Section 34. Immediately 
 north of this quartzite follows a porphyritic greenstone of tolerably fresh aspect. 
 This is exposed on the south side of the two knobs, which, on Dr. Rominger’s map, 
 lie to the southward of Deer Lake, to the east of the Carp River, and to the north of 
 the road. To the northward of this greenstone succeed first some greenish schistose 
 rocks without apparent agglomeratic character. These are represented by No. 12057. 
 These schists soon grade, however, both across the strike toward the north and in 
 the course of the strike toward the west, into a most strikingly conglomeratic rock, 
 which appears to make up about all the hills in the northern half of Section 33, be- 
 tween the quartzite and the road leading to the Ropes mine. 
 
 Specimen No. 12058 is an obscurely conglomeratic rock, collected about 150 steps 
 north of No. 12057. The conglomeratic character is best seen on a weathered sur- 
 face. A particularly fine exposure may be seen just west of Deer Lake furnace 
 (No. 12031). 
 
 Specimens No. 12029 are pebbles from a hold knob somewhat farther to the west. 
 From the same point came Nos. 12023 and 12024, representing the conglomerate 
 itself ; and Nos. 12025 and 12026, from two dikes two and one-half and ten feet wide 
 respectively. The smaller of these dikes cuts the conglomerate in a direction trans- 
 verse to its foliation, while the larger runs parallel to this structure. 
 
 Throughout the conglomerate there is a tendency to schistose structure, which, 
 however, is never very pronounced, and which varies considerably in its degree of 
 development. It seems to be rather the result of the intersection of close joints cut- 
 ting each other at a small angle than a true parallelism of structure. This foliation 
 stai ds about vertical and trends in an eastern and western direction. 
 
 The pebbles vary in size from such as are two feet in diameter down to minute 
 fragments. Pieces, less than six inches in length are most abundant. Occasionally 
 they appear well rounded, and this seems to be more particularly tbe case with tbe 
 larger sized pieces ; but more commonly they are sub-angular and flattened out in a 
 direction parallel to the schistose structure. On an exposed surface these pebbles 
 
186 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 stand out by virtue of tbeir whiter weathering. On a fresh fracture they are not 
 nearly so apparent, but seem to differ from the rest of the rock by their finer grain 
 and by their pinkish or greenish color ; the body of the rock having usually a dark 
 greenish gray tint. 
 
 No other kinds of pebbles were seen than those shown in the samples, which repre- 
 sent perhaps two phases : (1) A pinkish weathering felsitic (?) kind, and (2) a grayish 
 weathering greenish and more schistose kind. But this distinction, written on the 
 ground, seems hardly to be borne out by the specimens brought away. Certainly 
 those of the first named kind are more abundant. 
 
 Occasional schistose bands a few feet in width and quite free from pebbles may be 
 seen in the conglomerate, trending east and west. These, therefore, stand at a con- 
 siderable angle with the schistose structure. They are the only signs of a true bed- 
 ding in the rock, and if they do actually indicate a bedding are of very great im- 
 portance, both as showing a discordance between the bedding and schistosity and 
 also a nonconformity between these and the true bedded rocks lying just to the 
 south. Indeed, neither these doubtful bedding bands nor the schistose structure 
 perceptible in this conglomerate is concordant with the dip ofthe quartzite, which 
 is toward the south at a moderate angle. 
 
 North of the road leading to the Ropes mine the only rock noticed, for a short 
 distance, is represented by No. 12032, which does not show any conglomeratic struct- 
 ure, but which on the ground appeared very much like the pebbles in the conglom- 
 erate further south. 
 
 Still farther north, in the same township (T. 48 N., R. 27 W.), as, for instance, in 
 the middle and eastern part of Section 21, and again in the southwest quarter of Sec- 
 tion ?0, and in the northwest quarter of Section 29, to the north of Dr. Rominger’s 
 serpentine area (peridotite area of Plate I, herewith) are other very similar rocks. 
 Specimens 12036, 12037, and 12039 are from the SW £ of SYV £ Sec. 20, while No. 12043 
 is from the NW \ Sec. 29. Among the exposures from which this last specimen 
 was taken are some which seem to show the conglomeratic character of the Deer 
 Lake rocks. It is not positive, however, that the obscure markings which they 
 show are really those of pebbles. 
 
 Both the macroscopical and the microscopical examination of these 
 specimens show that they have been subjected to an intense strain or 
 stretching, which has resulted in the elongation of the component peb- 
 bles, and in the modification and partial recrystallization of the matrix, 
 after the manner shown in PI. XI, fig. 2, and in PI. XIV, fig. 2. Nev- 
 ertheless, the metamorphism attendant upon this dynamic action fortu- 
 nately has not been sufficient entirely to disguise the tuff nature of the 
 rock. In most cases this is still very apparent, and this occurrence is 
 therefore of great importance in confirming the conclusions reached with 
 regard to analogous, but more metamorphosed rocks, in the Marquette 
 and Negaunee areas. 
 
 We must regard these tuffs or agglomerates as originally composed 
 of the fine fragmental material of diabase. This consisted mainly of 
 triclinic feldspar and pyroxene, mingled with more or less amorphous 
 base, and stratified either by gravity or by the agency of water. In- 
 cluded in such a matrix were numerous true bombs of solid diabase and 
 ejected fragments of other rocks, mostly of a more acid character. 
 
 As is well known, material of this kind is of all the most liable to un- 
 dergo chemical alteration. This has been conclusively shown by the 
 observations of Captain Dutton, quoted above (p. 159). In consideration 
 
*\ r : S i ■ 
 
 ■ " willums. 1 AGGLOMERATES OF DEER LAKE. 187 
 
 of the great antiquity of the deposits here under discussion, therefore it 
 need excite no wonder that little of the original material now remains. 
 The rocks are largely composed of such secondary products as chlorite, 
 sericite, epidote, quartz, and calcite. All traces of original pyroxene, 
 or of possible olivine and glass, have wholly disappeared. The feldspar 
 * has, however, better retained its individuality. In some instances its 
 substance is still quite fresh ; and in others, where the substance is 
 changed, the form is still easily recognizable. The same class of altera- 
 tions has gone on in the solid portions of the agglomerates as in the 
 finely fragmental matrix. The more basic fragments produce chloritic, 
 the more acid sericitic, areas. Their original boundaries are, however, 
 for the most part, very distinct, often more so in the field, or in the 
 hand-specimen, than under the microscope. Where the dynamic action 
 has been most intense a schistose structure has been developed in the 
 fragments, which is quite continuous with that of the finer grained ma- 
 trix. This is accompanied by a distortion or elongation of the in- 
 cluded fragments, caused by crushing and recementing, whereby the 
 sharpness of their outline is destroyed, and an apparent transition to 
 the matrix is produced. 
 
 Specimen No. 12057, described in the notes as “a greenish schistose 
 rock without apparent agglomeratic character,” appears under the micro- 
 scope at first glance as a confused aggregate of chlorite, calcite, and 
 quartz, through which occasional large grains of yellowish green 
 epidote are scattered. Characteristic forms of ilmenite, with leucoxene, 
 some sericite, and delicate little rutile needles are also present. A 
 more careful study of this section reveals the indistinct outlines of lath- 
 shaped feldspars, which once formed the interlacing network of a 
 granular diabase. These are so disguised by the new products devel- 
 oped in them — chlorite, sericite, and epidote — that it is only by an 
 attentive examination with a low magnifying power that they can be 
 recognized. They are, however, undoubtedly present, and the rock 
 must therefore be regarded, not as a tuff, but as an extremely metamor- 
 phosed form of a massive flow, in which the profound chemical changes 
 and the development of a schistose structure progressed together. 
 
 Specimen No. 12058, “an obscurely conglomeratic rock collected 
 about 150 steps north of the locality of No. 12057,” bears in the hand- 
 specimen a close resemblance to the one last described, but under the 
 microscope its different character is at once apparent. The feldspar 
 substance is here less altered, and the rock is mostly composed of 
 minute crystals or fragments of crystals connected by that peculiar 
 aggregate of chlorite scales common in stretched basic rocks, where the 
 direction of the scales follows the schistose structure. (See PI. XI, 
 fig. 2.) Occasional larger fragments of feldspar crystals are scattered 
 through this finer mass, but these are always broken and irregular in 
 shape. The chloritic substance has doubtless originated from the py- 
 roxene or glass, while a vast number of the most delicate little rutile 
 
188 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 needles, arranged in long, sinuous bands, appears to represent the 
 original ilmenite. Calcite areas also occur. A narrow white vein 
 which traverses this hand-specimen possesses an interesting micro- 
 scopic structure. The little fissure was first coated with chalcedonic 
 quartz, and then with a layer of quartz crystals which projected their 
 terminations into the opening. These possess a perfect zonal structure, 
 due to the arrangement in successive layers of fluid inclusions. The 
 remainder of the space was subsequently filled with carbonate. 
 
 Specimen No. 12031, from a point a short distance west of where the 
 last mentioned pieces were collected, and Nos. 12023, 12024, 32029, and 
 12030, from another point still farther west, represent the agglomerate 
 in its most typical development, and leave no doubt as to its true 
 nature and origin. As in the specimens last mentioned, the matrix of 
 the rock is of a grayish green color and the grain is mostly aphanitic, 
 although frequent minute angular fragments may be detected by the 
 aid of a pocket lens. There is always a more or less pronounced folia- 
 tion developed in this matrix. The pebbles, which impart to the rock 
 its agglomeratic structure, show most distinctly on a weathered sur- 
 face. Here they present a white or pinkish gray color, which contrasts 
 most sharply with the pale green of the inclosing matrix. On a fresh 
 fracture the inclusions have a greenish gray color, but their compact, 
 fine grain, like^ that of halleflinta, serves to identify them where the 
 color fails. These massive felsitic fragments are of varying size and 
 angular or subangular in shape (rarely well rounded). They are dis- 
 tributed through the matrix indiscriminately, the longest axes being by 
 no means parallel, as we might expect in a sediment. The foliation of 
 the rock appears to have been produced by a great tension, which has 
 stretched the matrix and sometimes elongated the pebbles, sometimes 
 broken them, and sometimes forcibly torn the solidified matrix away 
 from them. The latter case is represented in Fig. 29, which represents 
 
 Fig. 29.— Weathered surface of a specimen of the Deer Lake agglomerate. 
 Natural size. No. 12023. 
 
 the appearance of a weathered surface on specimen No. 12023. It can 
 here be plainly seen that the longest axes of the pebbles stand almost 
 at right angles and that the matrix has been forcibly separated by the 
 stretching action, on each side of the central pebble. 
 
WILLIAMS.] MASSIVE DIABASE OF DEER LAKE. 189 
 
 The microscopical study of these specimens adds much to our knowl- 
 edge of the true structure of these agglomeratic rocks. 
 
 The matrix is found to be composed of very angular to subangular 
 fragments, extending down to the minutest size. These generally still 
 retain their form, although their original substance has undergone 
 change to chlorite, epidote, and calcite. Small feldspar crystals or 
 broken fragments of larger ones are scattered about, the substance of 
 which has been altered in varying degree. In the chlorite especially, 
 very sharp rutile needles abound. These seem to represent the titan- 
 ium of an original ilmenite. 
 
 Unmistakable evidence of clastic structure is everywhere encount- 
 ered; but this is not the clastic structure of a sediment. The angular 
 shape, different substance, and enormous variation in the size of frag- 
 ments lying side by side, all clearly indicate an agglomeration of vol- 
 canic detritus — and one, indeed, in which many of the original features 
 are admirably preserved. 
 
 Among the smallest of the included fragments, those resembling a 
 massive diabase in structure are not uncommon; but to judge from 
 the statement in the field notes quoted above, as well as from the 
 hand-specimens submitted to me for study, the larger “pebbles” or 
 fragments are mostly composed of the lighter and felsitic rock. This is 
 unfortunately too much altered to allow of a wholly satisfactory diag- 
 nosis. It may be best seen in section No. 12023, where it resembles a 
 porphyrite. The grouudmass still retains its ophitic structure, and 
 is filled with well formed porphyritic crystals of plagioclase. No 
 original quartz nor orthoclase could be detected ; one or two chloritic 
 areas, which must probably represent former augite or hornblende 
 crystals, were, however, observed. 
 
 Specimen No. 12025 represents a narrow, transverse dike of massive 
 greenstone, and No. 12026 a broader one of the same material, parallel 
 to the schistose foliation. Under the microscope both are typical, 
 though highly altered diabases. The former is aphanitic and has 
 only a very indistinct foliation in the hand-specimen. Under the 
 microscope the original structure is nearly obliterated ; still, traces of 
 it remain. Chlorite, calcite, quartz, and iron oxide are almost the only 
 mineral components. 
 
 The second, coarse grained diabase, is entirely massive in the hand- 
 specimen. It has an even green color, but cleavage surfaces of feld- 
 spar are frequent. Pyrite is also common in it. Under the microscope 
 the typical diabase structure is perfectly preserved. The texture is 
 quite coarse, and the feldspars mostly retain their twinning structure. 
 The rock has been stretched, and these feldspars are much broken and 
 have their fragments separated. The pyroxene is wholly altered to 
 chlorite, epidote, and calcite, and the ilmenite is accompanied by 
 leucoxene. 
 
 The rock occurring north of the road leading to the Ropes mine and 
 
190 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [bull. 62 . 
 
 directly west of Deer Lake, is devoid of conglomeratic structure. 
 (No. 12032.) In the field it was noted to have a resemblance to the 
 substance of the larger “ pebbles,” and this resemblance, to a certain 
 extent, is borne out by the- microscopical examination. The rock ap- 
 pears to be massive, and not a tuff; but it has been subjected to in- 
 tense crushing and stretching action. It is full of porphyritic crystals, 
 which are mostly altered to muscovite. The groundmass is principally 
 composed of small rectangular feldspar crystals. All, however, are 
 much broken and separated, and the interstices are filled with green 
 chlorite scales. The main difference between this rock and that form- 
 ing the compact felsitic pebbles in the agglomerate lies in the apparent 
 orthoclastic nature of the porphyritic feldspar crystals, and in the 
 chlorite which has been so abundantly developed in the groundmass. 
 
 The specimens from the more northerly areas, numbered 12036, 
 12037, 12030, and 12043, belong to the same category as those just 
 described. No. 12036 is a confused aggregate of feldspar fragments of 
 various sizes, together with some quartz and chlorite. Nos. 12039 and 
 12043 are almost too much altered to allow of any study. The former 
 is a mass of nearly opaque decomposition products, and the latter is an 
 almost continuous mat of sericite scales. No. 12037 alone appears like 
 a massive rock— most probably a fragment included in the tuff. It is 
 a hornblende granite, with but little quartz, composed principally of 
 idiomorphic feldspar. The minute green hornblende needles fill the 
 interstices between these square or rectangular crystals. 
 
 We may, therefore, consider the pyroclastic 1 nature of the Deer Lake 
 conglomerates as beyond any question. They represent volcauic de- 
 tritus, ejected by an explosive force at the earth’s surface. In this way 
 they form a most welcome but not unexpected support to the con- 
 clusions reached in regard to the other more highly altered rocks of 
 the same class occurring in the Marquette region. 
 
 The term “agglomerate” here applied to these rocks is one in gen- 
 eral usage among the English geologists 2 to designate a tumultuous 
 assemblage of volcanic ejectamenta — bombs, foreign blocks, etc., of all 
 sizes and shapes, cemented by a fine grained paste of volcanic ash. 
 
 The closest analogues to the Deer Lake rocks are the breccias, ag- 
 glomerates, and tuffs, described by Dr. A. Geikie from St. David’s, in 
 Wales. 3 This author says, p. 93: 
 
 The rocks of St. David’s present features of interest and importance, not only in 
 the palaeozoic history of Britain, but in regard to general theoretical questions. 
 They include, for example, perhaps the oldest group of lavas and tuffs, the relative 
 date of which is known. They have been subjected to a process of metamorphism 
 which has affected only certain beds or kinds of rock. They have been penetrated 
 by masses of granite and quartz porphyry, around which another kind of metainor- 
 phism has been manifested. At a later period they have been injected with diabase 
 dikes, etc. 
 
 1 J. J. H. Teall, Geol. Mag., London, 3d series, vol. 4, November, 1887, p. 493. 
 
 2 Cf. J A. Phillips, Quart. Jour. Geol. Soc., vol. 24, 1878, p. 476, and A. Geikie Text-Book of Geology, 
 1882, p. 163. 
 
 2 Quart. Jour. Geol. Soc., London, vol. 39, 1883. 
 
Williams.] AGGLOMERATES OF ST. DAVID’S, IN WALES. 191 
 
 All this might have been written to apply equally well to the rocks 
 occurring near Marquette. 
 
 With special reference to the tuffs, Dr. Geikie says : l 
 
 They vary likewise in texture from somewhat coarse breccias or agglomerates, 
 through many gradations, into fine silky schists in which the tufaceous character is 
 almost lost. Generally they are distinctly granular, presenting to the naked eye 
 abundant angular and subanglar lapilli, among which broken crystals of a white, 
 somewhat kaolinized feldspar and fragments of fine grained felsite are often con- 
 spicuous. 
 
 The matrix of these Welsh agglomerates appears to be generally 
 green, while the included lapilli or u pebbles” are sometimes basic in 
 character aud of a greenish color $ sometimes more acid, with a com- 
 pact structure and pinkish color. 
 
 Their resemblance is thus seen to be very close to the Deer Lake 
 agglomerates described in this chapter. 
 
 Quart. Jour. Geol. Soc. London, vol. 39, p. 295. 
 
CHAPTER VI. 
 
 GENERAL RESULTS AND CONCLUSIONS. 
 
 ORIGINAL CHARACTER OF THE MENOMINEE AND MARQUETTE GREEN- 
 STONE AREAS. 
 
 In speaking of the geology of the Menominee and Marquette regions 
 I refer, it must be understood, only to the greenstones and certain inti- 
 mately associated acid rocks. Ho attention was paid to the quartz- 
 ites, dolomites or shales of the younger, iron-bearing Huronian. With 
 a view of obtaining a clear idea of the primary nature of these rocks 
 we shall consider in succession : The evidence of their eruptive charac- 
 ter; their original types and mineralogical composition; the conditions 
 under which they were formed; and, finally, their succession in time. 
 
 EVIDENCE OF ERUPTIVE CHARACTER. 
 
 Field evidence . — This is more distinct in the case of the Menominee 
 greenstones on account of the simpler character of their exposures. 
 Here we find them extending in two comparatively narrow and nearly 
 parallel bands for a considerable distance. Their color, weight, text- 
 ure, and frequent massive structure are such as are associated with rocks 
 of igneous origin, while in some cases, as just below the Lower Quinne- 
 sec Falls, they project out of the surrounding schists in the form of a 
 high, precipitous ridge, suggestive only of a great dike. Although 
 successive layers of these rocks differ considerably in composition, and 
 though they possess within themselves well marked schistose varieties, 
 yet they are sharply defined against the adjoining Huronian beds, into 
 which they never pass by gradual transitions. Indeed, these rocks have 
 been considered by many of the geologists who have examined them 
 most carefulty as of eruptive origin. Those, on the other hand, who 
 have regarded them as either wholly or partially sedimentary have 
 been able, as far as I know, to cite only two arguments in favor of thei r 
 opinion. These are : First, the coincidence of the direction of these 
 bands, and of their alternating component members with the general 
 strike of all the rocks of this region ; and, second, the frequent con- 
 formity of the schistose structure in these bands to the bedding of the 
 adjacent sediments . 1 
 
 Let us, however, consider whether these two facts are not wholly in 
 accord with the supposition that these greenstones are of igneous origin. 
 
 This conformity is by no moans universal. 
 
 11)2 
 
WILLIAMS. ) 
 
 EVIDENCE OF ERUPTIVE CHARACTER. 
 
 193 
 
 If they were intrusive they would follow in their course the line of least 
 resistance, which would probably be the direction of the bedding of the 
 sediments. If, however, as seems from various considerations much 
 more probable, these greenstones belong to a formation older than the 
 Huronian, and if they were produced in the form of great igneous (and 
 perhaps submarine) overflows which composed the bottom of the basin 
 in which the iron-bearing sediments were subsequently deposited, then 
 the great lateral compression, which so contorted these sediments and 
 elevated them into their present almost vertical position, would have 
 brought the underlying greenstones at the same time into just the posi- 
 tion they now occupy. And if these greenstones had been formed as 
 successive flows, differing more or less in structure and composition, in 
 the process of upheaval they must have behaved like any other com- 
 plex of horizontal beds and have produced conformable members of the 
 series exposed in the Menominee valley, as is actually the case. 
 
 Now, also in regard to the second point of objection, if we admit that 
 massive rocks may have a schistose structure (like a slaty cleavage), 
 developed in them by pressure, then, in this case, the direction of this 
 cleavage, perpendicular to the action of the pressure, must agree with 
 the stratification of the now almost vertical sediments. 
 
 Nor is it necessary to assume that the schistosity of these rocks was 
 wholly produced at the same time with the crumpling and slaty cleav- 
 ages of the overlying detritals; since the same crumpling force may 
 have worked in the same direction at two widely separated periods. 
 Indeed, there is excellent reason to believe in two such periods, since 
 the dikes, which in the Marquette region penetrated the greenstone 
 schists subsequent to their being made schistose, have evidently them- 
 selves been subjected to further squeezing. These dikes appear to be 
 contemporaneous with the sheets of greenstone interfolded with the 
 detrital iron-bearing strata, which sheets themselves show a similar de- 
 gree of schistosity with the dikes referred to. In the Marquette region 
 there is generally a very noticeable difference as to the amounts of sec- 
 ondary cleavage in the greenstone schist area, and in the strata of the 
 overlying iron-bearing series, this being very much greater in the former 
 case. Coincident with this difference is the frequent gentle bowing of 
 the iron-bearing strata in this region, the dips of its layers being often 
 quite flat, while the cleavage of the green schists always stands at a 
 very high angle. In the Menominee region, on the other hand, the 
 folding of the iron-bearing series is very much closer and slaty cleavage 
 is much more generally developed. This would seem to indicate that 
 the second period of squeezing was more intense in the Menominee 
 area, and that it was, therefore, probably more instrumental in render- 
 ing the greenstones schistose here than in the Marquette region. 
 
 The arguments used by the defenders of the sedimentary origin of 
 the Menominee greenstones can not therefore be regarded as valid. 
 
 On the other hand we may cite, as positive evidence that the foliation 
 Bull. 62 13 
 
194 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 I BULL. 62. 
 
 of the greenstones is a secondary feature, the fact stated by Major 
 Brooks, that at the Four-Foot Fall this foliation is conformable to the 
 adjoining clay-slate, which has a “ stroug cleavage and no distinguish- 
 able bedding planes .” 1 Thus the schistose structure of the greenstone 
 now agrees with the secondary slaty-cleavage of the sediment, which, 
 of course, may or may not agree with its original bedding, since this 
 is here obliterated. Furthermore, what foliation the greenstones pos- 
 sess may be traced in almost every case into a jointing, or into bands 
 produced by the crushing attendant upon faulting and slipping, which 
 has taken place within the rock-mass. Finally, the abruptness with 
 which the foliation of the greenstones commences and breaks off in the 
 direction of the strike is wholly inconsistent witlr the theory that it is 
 due to original stratification. At the Four-Foot Fall, for instance, the 
 greenstones strike almost at right angles to the river, and yet they are 
 very schistose on the Wisconsin and very massive on the Michigan 
 bank. Such cases are not uncommon while even more difficult to ex- 
 plain are differences in the strike of schistose bands which traverse 
 a massive rock (like those observed at the Upper Twin Fall), unless we 
 assume that they were produced by a force which acted unevenly and 
 not in a constant direction. 
 
 The field evidence that the greenstones within the Marquette belt 
 are of igneous origin is not so plain as that encountered in the Menom- 
 inee valley. Although we find here unmistakable dikes of unal- 
 tered diabase and others of altered though still massive greenstone, 
 yet some of the most important of these rocks, especially in the north- 
 ern part of the Marquette area, are so regularly banded and stratified 
 that we are obliged to seek the agency of water to account for their 
 formation. Nevertheless, we are not obliged to separate even these 
 greenstones altogether from the igneous rocks which accompany them. 
 For reasons stated at length in Chapter IV, they may be most satis- 
 factorily explained as tuff deposits, half volcanic, half sedimentary, 
 which throw important light upon the physical conditions under which 
 the more massive rocks were produced. 
 
 Strong collateral evidence respecting the original nature of the green- 
 stones of both these areas may be obtained from a study of the acid rocks 
 which are quite constantly associated with them. The indications of 
 the eruptive character of these rocks are so unmistakable that it seems 
 to have hardly ever been doubted by any one who has examined them. 
 Large areas of granite occur on each side of the Huronian basins, both 
 in the Menominee valley and near Marquette, and dikes and apophyses, 
 presumably radiating from these main masses, penetrate the green- 
 stones for a considerable distance (cf. the Upper Quinnesec Fall, Horse 
 Eace, and region just north of Marquette). How, the composition of 
 these acid rocks is such that they resist chemical alteration much more 
 successfully than those of a more basic character. Hence we should 
 
 ‘■Geol. Wisconsin, vol. 3, p. 475. 
 
williams.] FIELD EVIDENCE OF ERUPTIVE CHARACTER. 
 
 195 
 
 expect to find their distinctively eruptive features, such as dike-form, 
 line of contact, original structure, etc., much better preserved. This is 
 the case, and yet these eruptive rocks often present phenomena of sec- 
 ondary foliation quite identical with those seen in the greenstones. 
 
 Near the southern end of the Brook Section, just west of Marquette, 
 this intrusive granite is filled with fragments of the surrounding schist 
 which it tore off while yet in a molten state. At the lower end of the 
 Horse Race Rapid, on the Menominee River, the acid dikes show a 
 marked diminution in the size of the grain toward the dike walls, a 
 structure eminently characteristic of rocks which have crystallized in 
 fissures. Near Upper Quinnesec Falls also was discovered a rock closely 
 resembling a granitic hornfels (No. 11064). But in spite of all the evi- 
 dence that the acid rocks are eruptive, their dikes, for the most part, 
 follow the strike of those through which they break, since this is the 
 line of least resistance, while many of them have a perfect foliation and 
 even a gneissic structure. What we may regard as satisfactory proof 
 that this foliation is a secondary feature may be seen at the head of the 
 Horse Race, where it conforms to the general strike of the surrounding 
 greenstones, even where this does not coincide, as is exceptionally the 
 case, with the sides of the acid band (see p. 115). A similar structure 
 has been observed by Prof. Oh. E. Weiss, of Berlin, near Thai, in Thu- 
 ringia and, like the present case, it may be regarded as certain evi- 
 dence that a schistose or even A banded structure may be developed in 
 acid dikes by secondary causes, independent of their own direction, 
 but conformable with the strike of the surrounding rocks. 
 
 Microscopical evidence . — The most convincing proof that the rocks of 
 the Menominee aud Marquette greenstone areas are of igneous origin 
 is not to be derived, however, from their field relations, but rather from 
 their microscopical structure. It is true that there are many cases 
 where rocks of widely dissimilar origin resemble one another so closely 
 that not even the minutest study of their internal structure is able to 
 distinguish them with certainty ; nevertheless there are in other cases 
 well marked peculiarities of structure which may be regarded as un- 
 failing indications that the rock possessing them has crystallized out of 
 a molten magma. 
 
 An explanation for these facts is not difficult to find. The original 
 structures of clastic and igneous rocks are characteristic and essentially 
 distinct. Where these remain there is no danger of confusion. In the 
 process of metamorphism, however, there is a constant tendency to ob- 
 literate the original features and to substitute for them certain second- 
 ary features. But these latter depend altogether upon the chemical 
 constitution of the mass and the nature of the metamorphosing forces, 
 and are independent of both the mineral composition and the structure 
 of the original rock. Hence it is that rocks fundamentally distinct in 
 
 1 Petrographiaclie Boitnige ana dem ndrdlicUen ThUringer Walde. Jahrbuch preuaa, gcol. Landes- 
 anstalt fur 1883, pp. 213-237. Berlin, 1884. 
 
196 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 . 
 
 both origin and structure grovr more and more alike when subject to 
 metamorphism. They may finally become indistinguishable and thus 
 their life histories may be lost, but so long as any trace of the original 
 structure is recognizable it may be relied upon as a safe guide. 
 
 It is, therefore, a matter of prime importance in petrography to be 
 thoroughly acquainted with original rock structures, and to understand 
 their significance. As a rule, those found in igneous rocks are more un- 
 mistakable than those which characterize clastic deposits. For instance, 
 universal observation, together with numerous synthetical experiments 
 in the laboratory, has shown that the peculiar divergent radial struct- 
 ure, known as the u ophitic v or u diabase ” structure, is always the 
 product of crystallization from a molten mass of certain basic rocks. 
 No single observation has ever been made to indicate that this structure 
 can originate in a sediment or by any metamorphism of a sediment 5 
 hence, we are justified, when we encounter the u ophitic” structure in 
 a rock (no matter how much it may otherwise resemble a sedimentary 
 deposit) in assuming that it is of igneous origin. Now, precisely this 
 characteristic structure is what we do meet most frequently in the 
 greenstones of both the Menominee and the Marquette area. Nor is it 
 alone in the most massive and apparently least altered specimens that 
 it is found ; often the most perfectly schistose of these green stones dis- 
 close it, and that, too, where none of the mineral components have 
 escaped complete alteration. 
 
 Other structures, scarcely less typical of an igneous origin are also 
 encountered in other of the Marquette and Menominee rocks. Some 
 of these are : porphyritic structure , with well defined crystals and even 
 a zonal growth ; micropegmatite and granophyre structure , in granite, 
 diorite and diabase ; poicilitic structure, shown by the hornblende in the 
 diorite porphyry at Lower Quiunesec Falls. The skeleton forms of the 
 acicular feldspar crystals, still recognizable in the aphanitic greenstones 
 of the Upper Twin Fail, as well as in thos*e of the southern Marquette 
 and Negaunee areas, are also strongly indicative of igneous, and per- 
 haps also of glassy rocks. 
 
 The evidence of eruptive origin afforded by the present mineral com- 
 ponents of the Marquette and Menominee rocks is not so satisfactory 
 as that based on their structure. Nor is this different from what we 
 should expect. Chemical metamorphism precedes structural metamor- 
 phism. Instances are frequent in both regions of the disappearance of 
 every original mineral, while the structure remains intact. If we except 
 the comparatively recent and unaltered diabases near Marquette, pyrox- 
 ene — that most characteristic of volcanic minerals — was hardly ever en- 
 countered except in the gabbro at Sturgeon Falls. We can, however, 
 assert with certainty that it was once present in many other rocks, 
 where it is now represented by the pale green hornblende into which it 
 so readily passes. Other species typical of igneous rocks, such as lath- 
 
GABRRO AND DIABASE. 
 
 WILLIAMS.] 
 
 19 ? 
 
 shaped labradorite crystals and ilmenite fringed with leucoxene, on the 
 other hand, are still met with in abundance. 
 
 With such evidence that the greenstones and associated acid rocks 
 of the Menominee and Marquette regions are igneous in their origin, 
 we may next inquire as to how many different types may still with cer- 
 tainty be recognized among them. In this section, whose effort it is 
 to reconstruct the original form of the greenstones, no reference will 
 be made to the secondary or metamorphic rock-types. 
 
 DIFFERENT ORIGINAL ROCK-TYPES. 
 
 BASIC' BOCKS. 
 
 Olivine Gabbro . — This type, containing abundant and perfectly crys- 
 tallized olivine, was found only in the northern area above Negaunee ; 
 (See Chap. V, p. 180); and even here under circumstances which left 
 doubt as to whether the exposure was in situ, or a part of a huge, buried 
 glacial bowlder. 
 
 Gabbro . — The only undoubted representatives of this type, i. e., gran- 
 ular aggregates of allotriom orphic diallage and plagioclase, were found 
 at Sturgeon Falls on the Menominee Eiver. Their diallage is of an 
 unusually pale color and, like the whole rock, remarkably poor in iron, 
 (cf. analysis on p. 76.) Their feldspar is almost wholly changed to 
 saussurite. The rock exposed near the Eureka shaft, two miles west 
 of Marquette, appears once to have belonged to this same type (p. 70); 
 while the granular diorites so common at the Quinnesec Falls, although 
 they now contain only pale green hornblende and no diallage, agree so 
 closely with the Sturgeon Falls rock in appearance, structure, and chem- 
 ical composition, that it is very probable that they were once gabbros 
 also (pp. 86, 102). 
 
 Diabase . — This is by far the most common rock-type and it is found 
 in every variety and stage of alteration. 
 
 An unaltered olivine diabase is the youngest rock of the Marquette 
 area. It intersects all the other greenstones as well as the granite, as 
 may be'seeu at the mouth of Dead Eiver, besides occurring in inter- 
 bedded sheets in the iron bearing series itself. It forms the great dike 
 which terminates at Lighthouse Point, as well as many other smaller 
 ones exposed in the Brook Section, in the northern area and at other 
 localities. As the olivine is the first of all minerals to disappear, this 
 type can, of course, be recognized only in the freshest specimens. 
 
 It is not always possible to say positively whether the quartz in the 
 diabase is an original or a secondary constituent. The formor, how- 
 ever, is probably the case in certain very fresh specimens and where, 
 as in No. 11675 from the great dike, and No. 11646 from Front street, 
 Marquette, it is present as a micropegmatitic intergrowtli with the 
 feldspar (p. 141). 
 
 No non-olivinitie diabase was discovered in a perfectly fresh state, but 
 this type is assumed for many occurrences in which alteration is more or 
 
198 greenstone schist areas of Michigan. I BULL. 62. 
 
 less advanced. Such an assumption mast, however, be doubtful, since 
 any original olivine would have been the first mineral to disappear. 
 
 Diabase Porphyry .• — It is now impossible to say whether the porphy- 
 ritic greenstones occurring at the western end of the ridge below the 
 Lower Quiunesec Falls once belonged to this type or not. If they did, 
 they contained considerable original brown hornblende as an accessory 
 constituent; but it seems more probable that these rocks were diorites. 
 
 Glassy Diabase and Melaphyre. — From the sides of the unaltered dia- 
 base dikes, glassy and half glassy rocks were obtained, which, of 
 course, represent only a local facies of the main mass, due to more rapid 
 cooling. They contain incomplete and skeleton forms of the minerals 
 which were the first to crystallize, and in this respect they closely re- 
 semble some of the aphanitic greenstones of the southern Marquette 
 and Negaunee areas. Indeed, one of these half glassy rocks from the 
 edge of a much altered dike in the Brook Section, near Marquette (No, 
 11680, see p. 144), is quite identical with a certain widespread variety of 
 the fine grained greenstones, and gives perhaps the clew for the decipher- 
 ing of their original form (cf. p. 163). 
 
 . Diorite. — The readiness with which the i^roxeue of eruptive rocks 
 passes over into a corresponding amphibole, makes the number of dior- 
 ites among the Menominee and Marquette greenstones appear much 
 larger than it really is. A majority of these are undoubtedly of second- 
 ary origin, having been derived from pyroxene rocks. Nevertheless, 
 others of them, in which the secondary hornblende can be traced back 
 into a compact brown variety of the same mineral, must be regarded as 
 true diorites, unless we make the assumption that pyroxene has passed 
 by paramorphism first into basaltic, and subsequently into fibrous green 
 hornblende. The origin of other of the dioritic greenstones must 
 always remain uncertain. Even at the risk of including some rocks of 
 secondary origin, the principal dioritic types may be enumerated as fol- 
 lows : Gabbro type — light colored, granular rocks, like those forming the 
 barrier at Upper Quiunesec Falls ; these so closely resemble the Stur- 
 geon Falls gabbro (even down to the orthopinacoidal parting\of their 
 hornblende) that there is strong reason to believe that they have been 
 derived from a similar rock. Coarse grained diorite of the Horse Race, 
 with idiomorphic feldspar and a pale green hornblende, which, though 
 itseif secondary, has probably been formed from a compact variety of 
 the same species. Granular diorite , like No. 11175 from Four-Foot Falls 
 and several dike-rocks in the Negaunee and Northern areas. Quartz 
 diorite, like the Picuic Island rock and No. 1 1 S3 J , from the Northern 
 area, west of Marquette. (See Plate IX, fig. 2.) Both of these are per- 
 haps more properly amphibole granites, although the relative propor- 
 tions of their orthoclase and triclinic feldspar leaves this indoubt. The 
 so-called u epidiorites v are undoubtedly of secondary origin, and have 
 been derived generally from augitic rocks. 
 
WILLIAMS.] 
 
 ORIGINAL MINERAL CONSTITUENTS. 
 
 199 
 
 Biorite Porphyry . — The rocks containing large poicilitic hornblende 
 crystals, collected from the western end of the ridge below the Little 
 Quiunesec Falls, which have already been mentioned under the head of 
 Diabase Porphyry, although they should perhaps receive the above 
 designation. 
 
 Tuffs. — The schistose, banded greenstones which compose so large a 
 part of the northern Marquette area are found to be best explained as 
 tuff deposits of the basic eruptives which accompany them. 
 
 ACID ROCKS. 
 
 Granite. — Each of the greenstone areas is bounded on both the north 
 and south by a large mass of granite. This rock is a typical granitite 
 as can be best seen from the specimens collected south of the Horse 
 Pace in the Menominee Yallev and north of the Marquette greenstone 
 belt. Muscovite granite occurs in some of the bosses near Marquette, 
 notably at the so called u gold mine 99 near Pine street. Amphibole 
 granite is possibly represented in the specimens from Picnic Islands and 
 the Northern area which have already been mentioned under the head 
 of Quartz Diorite, although they appear to occupy a position midway 
 between these two types. 
 
 Granite Porphyry and Quartz Porphyry are the forms assumed by the 
 granite where it penetrates the greenstones in dikes or apophyses. 
 They are abundant in both areas and are united by a continuous series 
 of transitional forms. These rocks are among the most interesting ones 
 anywhere met with on account of the perfection with which they show 
 the effects of dynamic action. By either stretching or compression 
 they are changed into Augen gneiss or schistose porphyry, both of which 
 retain in their microscopic structure very plain evidence of the manner 
 in which they were produced. 
 
 ORIGINAL MINERAL CONSTITUENTS. 
 
 Orthoclase occurs in all the acid rocks — granites, and porphyries $ in 
 some of the fragmental rock, as, for instance, those near Iron Mount- 
 ain and in the stretched tuffs on the Carp River north of Teal Lake, 
 and probably in the Picnic Island rock north of Marquette. 
 
 Microcline. — It is doubtful whether this form of potash feldspar is 
 ever original. In some cases at least it is certainly the result of intense 
 dynamic action on rocks already solid. 
 
 Oligoclase is, in all probability, the species of striated feldspar occur- 
 ring in the granites. 
 
 Lahradorice is the prevailing original feldspar in all the greenstones, 
 as it is in the unaltered diabases occuring near Marquette. 
 
 Quartz is an abundant component of all the acid types \ and it occurs 
 also in both diorites and diabases, although it is here not always pos- 
 sible to distinguish between what is original and what is secondary. 
 
 Muscovite seems to exist in one or two granites as a primary compo- 
 nent, but in the majority of cases it is a derivative of the orthoclase. 
 
200 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 {bull. 62 . 
 
 Biotite is abundant in the granites. It is also present in the diorites, 
 especially in those from the Horse Race Rapid, although here It may 
 be secondarily developed out of the hornblende. In the diabase it is 
 sometimes seen forming a border around the ilmenite. 
 
 Hornblende . — Compact brown, or basaltic hornblende is common in 
 very many of the greenstones, though mostly as remnants of crystals 
 which have become partly green or fibrous. It is also present in the 
 Sturgeon Falls gabbro and in the Marquette olivine diabase. Compact 
 green hornblende is also a very common mineral in the greenstones, but 
 it impossible to tell to how great a degree this may be of secondary origi n. 
 
 .Diallage of a very pale color and very poor in iron is abundant in the 
 gabbro of Sturgeon Falls. (See PI. YHI, fig. 1.) 
 
 Augite of the ordinary kind, having a reddish brown color in trans- 
 mitted light, is an essential ingredient of all the fresher diabases ; and 
 often exists as a core in the center of partially uralitized crystals. 
 
 Olivine , in fresh and perfectly formed crystals, was found in the oli- 
 vine gabbro of doubtful origin which occurred in the Northern area 
 above Negaunee. It also once formed a component of the younger dia- 
 bases near Marquette, although it is now so altered to serpentine as to 
 be, only recognizable by its form. 
 
 Zircon is abundant in nearly all the acid rocks, and is present in the 
 sediments near Iron Mountain in the Menominee valley. (No. 11113.) 
 
 Apatite is universal in all the rocks which have not been sufficiently 
 altered to obscure it. 
 
 Tourmaline is common in the more acid rocks. It may be best seen 
 in the granite and acid dikes near the Horse Race and Upper Quinue- 
 sec Falls. It is also present in the sediments exposed near Iron Mount- 
 ain and Four-Foot Falls, as well as in the hornfels (No. 11064.) 
 
 S phene occurs in both granite and diorite, especially in association 
 with hornblende. In some instances it seems to have been derived 
 from the alteration of ilmenite. 
 
 Orihite ( Allanite ) is present in certain granites, both near the Horse 
 Race and in the Northern area above Negaunee. 
 
 Ilmenite and Magnetite . — The opaque iron oxide minerals are present 
 in all the rocks in their usual abundance. Ilmenite is the most fre- 
 quent, especially in the greenstones, but magnetite is also present. 
 
 CONDITIONS UNDER WHICH THE GREENSTONES WERE FORMED. 
 
 There is considerable evidence to show that the greenstones, both of 
 the Menominee and the Marquette region, solidified at the surface, 
 under subaerial or subaqueous conditions. 
 
 In the Menominee Valley this evidence consists (1) of the fine text- 
 ure of the rocks ; and (2) of the alternation of bands of different types, 
 which probably in their original position represented successive flows. 
 Finenessof grain is universal in the Menominee greenstones, and we may 
 be certain that it was a primary feature in spite of the extensive alter- 
 
WILLIAMS.] 
 
 MACROSTRUCTURAL METAMORPHISM. 
 
 201 
 
 ation of these rocks. Tt is especially noticeable in the case of the gab- 
 bro, which is almost always a coarse grained rock when it has solidified 
 at any depth. The succession of massive beds, like the pale gabbros 
 and the dark diabases seen at Lower Quinnesec Falls, are difficult 
 to account for except by supposing that they were once horizontal 
 sheets which flowed one over another and which were subsequently ele- 
 vated into their present nearly vertical position. Traces of tuff mate- 
 rial are not as distinct here as in the Marquette region, although indi- 
 cations of their existence are by no means wanting. We might reason- 
 ably expect that any original scoriaceous or amygdaloidal structure 
 would have disappeared in the course of the profound chemical changes 
 through Which these greenstones have passed. 
 
 In the Marquette area proof of the superficial origin of the green- 
 stones may be found (1) in the fineness of grain, and (2) in the frag- 
 mental detritus or tuff, such as would accompany volcanic action. The 
 so called u aphanitic greenstones,” which play so important a role in the 
 southern Marquette and Xegaunee districts, have traces of a structure 
 like that of a porphyrite or melapbyre (see PI. X, fig. 2). At least 
 there are incomplete forms of feldspar crystals apparently imbedded in 
 a groundmass which might easily have originated from the devitrifica- 
 tion and decomposition of a cryptocrystalline or even glassy base. The 
 finely banded greenstone schists occupying the northern portion of the 
 Marquette belt present such strong evidence of stratification and such 
 peculiarities of microscopic structure (see PI XVI, fig. 1) that they are 
 best explained as tuff deposits belonging to the massive basic rocks. 
 The presence of fragmental material of this kind, of course, strongly 
 indicates surface origin for all these greenstones. Still other signs 
 point in the same direction. At least one well marked specimen of 
 amygdaloidal structure (Xo. 11746) was found near Baldwin’s Kilns, but 
 in the present highly altered condition of these rocks it can only occa- 
 sion surprise that even this was preserved. 
 
 MACROSTRUCTURAL METAMORPHISM OF THE MENOMINEE AND MAR- 
 QUETTE MASSIVE ROCKS. 
 
 This embraces all modifications in the structure of the massive rocks 
 produced by dynamic agencies and plainly visible to the unaided eye. 
 Such changes consist for the most part in the production of a banding, 
 foliation, or schistose structure, which tend to make the eruptive rocks 
 resemble stratified deposits. They are a secondary feature and must 
 be correlated with the slaty cleavage, not with the original bedding of 
 sediments. 
 
 Inthe process of upheaval and folding rocks may be subjected to great 
 compression, with more or less attendant shearing or faulting, or the re- 
 verse may be true and a tension result. In the first case foliation is 
 produced ; in the second, the phenomena of stretching. 
 
202 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [hull. 62 . 
 
 MACRQ8TRUCTURAL METAMORPHISM THROUGH COMPRESSION, FAULTING, OR CRUSHING. 
 
 Simple compression . — There seems to be no doubt that a foliation or 
 slaty cleavage may be produced by pressure in massive as well as in 
 stratified rocks. This cleavage is developed in all cases at right 
 angles to the direction of the pressure. It is particularly frequent in 
 such basic eruptive rocks as, by their chemical composition, are more 
 subject to alteration. In these the secondary development of such 
 cleavable minerals as chlorite, hornblende, sericite, and biotite, which 
 are given a parallel arrangement by crystallizing under pressure, 
 s f rongly conduces to the production of a schistose structure. The 
 pressure accelerates the chemical action, and may in this way de- 
 velop a schistose out of a massive rock without movement in the mass. 
 
 A very general feature in the foliated greenstones of both the Me- 
 nominee and Marquette regions is their tendency to cleave parallel to 
 a line instead of parallel to a plane; in other words, they possess a 
 dip but no decided strike. The rock then breaks with readiness into 
 loug rhomboidal prisms with almost any angle, but is severed with 
 difficulty at right angles to this axis of foliation. Such a structure 
 would seem to indicate the action of an unequal or shifting pressure. 
 Examples of this method of parting are very common, especially at 
 Sturgeon, Lower Quinnesec, and Twin Falls, in the Menominee Valley, 
 and in the southern portion of the Marquette greenstone area. 
 
 One of the best proofs of the secondary origin through dynamic 
 agency of the greenstone foliation is the fact, noticed by Major Brooks, 
 that at Four-Foot Falls this is parallel to the slaty cleavage, but not to 
 the bedding of adjoining sediments. 
 
 Another method by which a schistose structure is produced in the Me- 
 nominee greenstones, is the gradual flattening of the rhomboidal prisms 
 which are formed by the intersection of two sets of joint-planes. This 
 is illustrated by Figs. 20, 21, and 22, on page 128. These prisms seem 
 to be elongated by the action of intense pressure into a series of inter- 
 lacing lenses. A sort of “ Flaser 77 structure is thus produced which, in 
 its extreme development, becomes a well characterized schistose struct, 
 ure. Even in the broadest of these prisms a latent cleavage is often 
 noticeable parallel to their longest diagonal, always following the 
 general strike of the adjoining rocks. This structure, which I have 
 designated as rhomboidal, or diamond parting, may best be seen at the 
 Twin Falls or at the upper end of the great greenstone ridge below 
 Lower Quinnesec Falls. 
 
 Faulting or crushing . — A schistose structure is always produced in 
 massive rocks along lines where a great tension has been relieved by 
 breaking and a consequent displacement. Movement of this kind within 
 a solid mass, must be accompanied by more or less intense crushing, 
 and this allows increased circulation and lienee of the rapid production 
 of secondary crystallizations. Admirable instances of this phenom- 
 
WILLIAMS. ] 
 
 FAULTING OR CRUSHING. 
 
 203 
 
 euou abouud in both the Menominee and Marquette greenstones. At 
 the Sturgeon Falls, along the basin just below Lower Quiunesec Falls ? 
 below the Horse Bace, at the Twin Falls, at the foot of Arch street, 
 Marquette, and at many other localities within this area, it maybe seen 
 with remarkable distinctness. The exact effect of the crushing on the 
 original mineral constituents is visible only under the microscope and 
 hence will be considered in the succeeding chapter ; but any one who 
 will carefully examine any of the above named localities can not fail to 
 be convinced of the continuity and original identity of the massive and 
 schistose rocks. 
 
 Both the width of these schistose blinds and the intensity of the 
 crushing which they exhibit vary widely in different cases. Their di. 
 rection almost always coincides with the general strike, although at 
 Upper Twin Falls such bands were observed to have a different direc- 
 tion. (Seep. 132.) 
 
 This pulverization of the rock is accompanied by greatly increased 
 chemical action (except in the notable instance of the feldspar) and the 
 abundant production of chlorite. Such crushed bands possess a more 
 or less perfect lenticular or u Flaser ” structure, which passes gradually 
 into a lamination where the action has been more intense. This is al- 
 most entirely due to the parallel arrangement of the secondary chlorite 
 scales, so that we have a basic eruptive rock developing into a typical 
 chlorite schist. 
 
 Excellent examples of a massive, though much altered greenstone 
 fraying out into a chlorite schist by the action of a shearing force along 
 lines of slight displacement, were found at lower Twin Falls, and are 
 illustrated in Figs. 23 and 24. (See pp. 129, 130.) 
 
 The great mechanical force generated in the course of orographic 
 movements, aided by chemical action, sometimes develops schistose 
 bands in massive rocks, which wind around and encircle compact cores. 
 These are spheroidal or lenticular in shape, and seem for some unknown 
 reason to have better resisted the metamorphosing influences. A tine 
 example of this kind may be seen on the Wisconsin side of the Menom- 
 inee Eiver, just at the foot of Lower Quinnesec Falls. It is repre- 
 sented by specimens ]STos. 11017 to 11020, described on p. 93. Other 
 examples of the same kind occur in the railroad cut near Front street, 
 Marquette. 
 
 This last described structure has much in common with the spheroidal 
 or lenticular parting observed in the aphanitic greenstones of the south- 
 ern Marquette and Negaunee areas. (See Figs. 26 and 27, pp. 166, 177.) 
 Near the mouth of Whetstone Brook $ in the neighborhood of Bald- 
 win’s Kilns, and between Teal Lake and the Carp. Eiver, we see the tine- 
 grained greenstones broken up into circular or oval areas, which are 
 separated by a finer schistose matrix. This structure is common 
 through the Northwest, and has been termed by the Canadian geolo- 
 gists “concretionary trap.” It is, however, in no sense really concre- 
 
204 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 tionary, bat must be ascribed either to contraction which frequently 
 produces a perlitic structure or spheroidal parting in volcanic rocks, or 
 to a mechanical brecciation and rubbing together of the disjointed 
 fragments, as was found by Rothpletz to be the case in similar green- 
 stone schists of Saxony. (See p. 167.) 
 
 MACROSTRUCTURAL METAMORPHISM THROUGH STRETCHING. 
 
 The effect of stretching upon rock masses has only recently come to 
 engage the attention of geologists. It is evident that in the process of 
 the upheaval or folding some parts of the mass must be strained, while 
 other parts are compressed. As Heim first pointed out, such a tension 
 is relieved sometimes with and sometimes without a visible rupture. 
 Both of these methods are well illustrated in the massive rocks of the 
 Menominee and Marquette regions. 
 
 In the first case we find the formation of irregular, ragged seams, 
 which Heim has designated as gaping rents (“ klaffende Risse”), and 
 which I have termed u cross-gashes,” from their being torn open in a 
 direction perpendicular to that in which the tension was exerted. They 
 are, therefore, approximately parallel, and may produce a rough sort 
 of schistose structure. These seams sometimes remain open, but are 
 sometimes filled with secondary crystallizations, like quartz, calcite, or 
 chlorite, often with epidote. They are best exhibited in the great 
 greenstone ridge which extends along the river’s left bank below Lower 
 Quinnesec Falls. Their appearance, as far as it can be shown in a hand- 
 specimen, is represented in Fig. 10, p. 81. 
 
 The manner in which the round cores of the spheroidally parted 
 greenstones in some cases have been drawn out into interlacing lenses, 
 has already been noted (p. 177). 
 
 Stretching action may sometimes produce a banding in massive rocks. 
 This is especially the case with acid types, like granite and quartz por- 
 phyry. Examples of this are to be found among the acid dikes near 
 the Horse Race and in the vicinity of Marquette, but the most indubi- 
 table evidence of stretching in these rocks is contained in their micro- 
 scopic structure, and must therefore be reserved for description in the 
 following section. 
 
 MICROSTRUCTURAL METAMORPHISM OF THE MENOMINEE AND MAR- 
 QUETTE MASSIVE ROCKS. 
 
 Where profound mechanical and chemical changes have gone on si- 
 multaneously in rock masses, the final product may be wholly different 
 from the original starting point. Sedimentary and eruptive rocks seem 
 to approach each other more and more nearly, the longer they are ex- 
 posed to the same metamorphosing influences. In many cases the deri- 
 vation of certain schists can never be definitely settled ; in other cases, 
 however, where the field evidence is insufficient to decide, the micro- 
 
WILLIAMS.] 
 
 EFFECT OF DYNAMIC ACTION. 
 
 205 
 
 scope may yield reliable data for settling the origin of doubtful crystal- 
 line schists. Characteristic minerals or structures may often be de- 
 tected under the microscope after every original feature visible to the 
 unaided eye has been obliterated. 
 
 In stating the results of dynamic action observed with a microscope 
 in the Lake Superior rocks, we may speak first of the effect upon individ- 
 ual minerals, and then of new structures produced. As a rule, those 
 minerals and rocks which are hardest and most brittle are found to 
 exhibit these mechanical effects most perfectly. 
 
 EFFECTS OF DYNAMIC ACTION ON INDIVIDUAL MINERALS. 
 
 Quartz .— We find corroborative evidence of the fact stated by others 
 that quartz is frequently more sensitive to pressure than feldspar. In 
 the quartz porphyry, No. 11707, for instance (see PI. XY, fig. 2), 
 which has undergone a violent stretching, the feldspar crystals appar- 
 ently exhibit no resultant phenomena, if we except the presence in their 
 center of microcline as a possible product of strain ; the quartz crystals, 
 on the other hand, show' an unusual amount of deformation. In some 
 cases they are pinched out into pear or spindle shaped areas with an 
 undulatory extinction ; while in other cases they are much more 
 elongated, but show that this result has not been reached without a 
 crushing and displacement of their original substance (granulation). 
 The fragments are converted into a mosaic of interlocking grains by the 
 readiness with which silica is dissolved and deposited. Quartz that is 
 more or less optically disturbed is almost universal in the acid rocks 
 examined, showing that hardly any of them have been entirely free from 
 mechanical strains. That the quartz grains in the granite No. 11104 
 are not all original is proved by the little tourmaline crystal, which is 
 fractured and faulted at the junction of two of them, as depicted in Fig. 
 13, p. 112. 
 
 Feldspar . — The first effect of strain on feldspar is to produce an un- 
 dulatory extinction. This cannot, however, be carried as far as it is in 
 quartz, because the tension is here able to relieve itself by molecular 
 movements and the consequent formation of twinning lamellm. Sev- 
 eral cases were encountered where the gridiron or microcline structure 
 appears to have been secondarily developed in a potash feldspar by 
 this means, as in the granites Nos. 11104 and 11710 and in the schist- 
 ose quartz porphyry No. 11707. Such a production of secondary or 
 strain lamellae in the triclinic feldspars is by no means unusual. 
 
 Where the mechanical action is too intense to produce mere optical 
 disturbance or molecular gliding without rupture, the force of cohe- 
 sion is entirely overcome and the feldspar is fissured or crushed. In 
 case the force is exerted as a tension, the fragments thus formed are 
 separated, and the spaces between them are filled with secondary crys- 
 tallizations, especially chlorite. In other cases the fragments are merely 
 faulted against one another. Such examples of stretched and faulted 
 feldspar are very abundant in the schistose greenstones and acid rocks 
 
206 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62 
 
 of tlie Menominee and Marquette districts. It is generally possible to 
 recognize what fragments once belonged together, as may be seen by 
 an inspection of PI. IX, fig. 2, PI. XI, fig. 2, PI. X1Y, figs. 1 and 2, and 
 Fig. 11 on p. 105. Even in very schistose rocks, which are in other re- 
 spects chemically much altered, these broken feldspars are, as a rule, 
 unexpectedly fresh ; a fact which will receive particular attention in the 
 succeeding section. 
 
 If the mechanical force is still greater, a pulverizing or granulation of 
 the feldspar ensues. This is always accompanied by chemical action, 
 consisting of more or less complete solution and recrystallization. In 
 this way the substance is molded into new forms, which accord better 
 with the existing strains. 
 
 Such a partial grauulation of a large porphyritic feldspar crystal, pro- 
 ducing one of the lenticular u Augen ” of the metamorphic gneisses of 
 the Horse Eace, is shown in PI. XY, fig. 1. 
 
 In the process of feldspar granulation the calcium is frequently re- 
 moved, and the secondary mosaic is largely composed of albite, as was 
 first shown by Lossen. 
 
 Pyroxene . — Diallage is very subject to mechanical deformation. On 
 „ account of its relative softness and flexibility this consists mostly of the 
 bending or twisting of the crystals, or in the occasional production of 
 twinning lamellae. These phenomena may be well seen in the almost 
 colorless diallage of the Sturgeon Falls gabbro. Pyroxeue exists in no 
 other of the rocks examined except in those which are too young to 
 show any effects whatever of dynamic action. 
 
 Hornblende .— Certainly in a large majority and possibly in all the 
 rocks which I have studied from northern Michigan, hornblende is a 
 secondary product ; since, then, it is a result of metamorphism, it is not 
 strange that we rarely see in it the effects of that mechanical action 
 which caused the metamorphism. 
 
 Mica . — On account of its flexibility mica, like diallage, would be well 
 fitted to exhibit mechanical phenomena ; but the fact that, like the 
 hornblende, it is mostly a secondary mineral in those rocks to which 
 we have here devoted our attention, prevents such deformations from 
 being common. 
 
 Zircon , Tourmaline, etc . — These minute products of the first crystalli- 
 zation in the rock are often found to be broken or faulted by mechani- 
 cal action, as is shown in Fig. 13, p. 112, and Fig. 18, p. 122. 
 
 Ilmenite . — The iron minerals, on account of their opacity, of course 
 can exhibit no optical disturbance, but their grains are frequently torn 
 apart just like the feldspar crystals. This has been described in num- 
 erous instances, and it is represented in PI. XI, fig. 2. 
 
 NEW STRUCTURES PRODUCED BY DYNAMIC ACTION. 
 
 Whenever the crushing of rocks by dynamic agencies is accompanied, 
 as it almost always is, by chemical action and the production of new* 
 minerals, these must arrange themselves in accordance with the exist* 
 
 
WILLIAMS.] 
 
 NEW STRUCTURES BY DYNAMIC ACTION. 
 
 207 
 
 ing strains. These secondary minerals are such as themselves possess 
 a very perfect cleavage; their production, therefore, under circumstances 
 of uniform and continued strain, will naturally impart a foliation to 
 the originally massive rock. Nor is this all. The relief of the strain 
 and the consequent crushing of the rock will take place along certain 
 planes much more completely than along others; hence in these planes 
 the secondary minerals will be more abundant, and a banding of a once 
 homogeneous rock may result. 
 
 The final structures produced in this manner depend not altogether 
 upon the force exerted, but also upon the primary structure of the rock. 
 
 The rubbing together of individual crystal grains, the adhesion be- 
 tween which is weaker than their own internal cohesion, may produce 
 a pulverizing only around the edge, when the force is not too intense. 
 This phenomenon, to which Professor Kjerulf has applied the term 
 “peripheral granulation” (randliche Kataklase), 1 may bring about a 
 sort of pseudo-porphyritic structure, in which, however the porphvritic 
 crystals are only the larger remnants of the former grains without a 
 crystal form of their own ; or, if the crushing has been less, the grains 
 may appear to be held together by a fine granular cement, like the 
 stoues of a wall by their mortar. Hence Professor Tornebohm has 
 spoken of this as the “mortar structure” (Mortel Structur). 2 Many 
 admirable examples of these structures are to be seen in the Menominee 
 and Marquette rocks, especially in those of an acid character. There 
 may be particularly mentioned the granite from the great area south 
 of the Menominee, No. 11104; Nos. 11189 and 11190 from acid dikes at 
 the Horse Pace; Nos. 11678 and 11710 from the Brook Section, near 
 Marquette. In the first instance, a distinct micropegmatitic structure 
 is a noticeable feature of the granular cement. 
 
 If the original structure of the rock was porphyritic instead of 
 granitic, we find corresponding differences in the result. The ground- 
 mass is made schistose by the development out of its feldspar of sericite 
 or chlorite. The porphyritic crystals are more or less granulated, but 
 the secondary mosaic thus formed is often coarser in grain than the 
 groundmass. This is arranged around the remnant of the original 
 crystal in a lenticular area known as the “eye,” or “Auge,”iu rocks 
 called by the Germans, on account of this structure, Augengneiss. (See 
 PI. XV, fig. 1.) Unusually beautiful examples of this kind are to be 
 found among the acid dikes along the shores of the Horse Race — 
 especially specimens numbered 11184 and 11196. In some of the 
 schists which have been derived from the Sturgeon Falls gabbros a sim- 
 ilar structure is present. 
 
 Where secondary micaceous minerals have been developed in sinuous 
 bands which interlace and twine about abundant oval cores, a lenticu- 
 
 1 Grmidfjeldsprofilet ved Mjoaens sj dende. Nyt Mag. for Naturvidcnskabemo, vol. 29, p. 215, 1885 
 (Nenes Jalirbuch fiir Mineral., 1886, vol. 2, Referate, p. 244.) 
 
 ’Nigra ord om granit och gneis. Geol. Foren. Stockholm Forhandl, vol. 5, pp. 233-248. (Neues, 
 Jahrbuch fiir Mineral., 1881, vol. 2, Referate, p. 50.) 
 
208 
 
 GREENSTONE SCHIST AREAS OP MICHIGAN. 
 
 [BULL. 62 . 
 
 lar structure is produced, in which there is no contrast between ground- 
 mass and porphyritic crystals. This is called by the Germans “ Flaser 7 ’ 
 structure, a term which may advantageously be transferred to the Eng- 
 lish. It is often the case that a structure of this kind is so fine as to be 
 visible only under the microscope, when the designation “ microflaser 
 structure” is applicable. Examples of this lenticular interlaciug are 
 abundant in the schistose greenstones of northern Michigan. It is es- 
 pecially typical in the Sturgeon Falls schists, and in those at Lower 
 Quiunesec Falls ; it may also be well seen in the granite at the mouth 
 of the Dead Fiver, north of Marquette. 
 
 In rocks that have been subjected to a great tension, a peculiar micro- 
 scopical structure has been developed, caused by the rupture of the 
 original crystals and a pulling apart of their fragments. Between these 
 chlorite is formed, the scales of which are parallel to one another and 
 to the direction of the stretching. This chlorite appears to have re- 
 sulted from the recrystallization of the substance of the original bisili- 
 cates, since no trace of these now remains, although the broken feldspar 
 is always remarkably fresh. There must be something in the dynamic 
 action of an intense tension particularly conducive to the formation of 
 tips chlorite, for exactly this modification of this mineral was not en- 
 countered in rocks produced in any other way. Its presence, of course, 
 brings out a decided schistose structure. Excellent examples of this 
 phase of structural metamorphism abound in the Menominee and Mar- 
 quette greenstones, although I do not know that anything exactly like 
 it (particularly when taken in connection with the remarkable freedom 
 of the broken feldspar from all signs of chemical change) has ever been 
 described before. It is illustrated in PI. XI, fig. 2. The widely dif- 
 ferent results produced in the same greenstone by chemical action alone 
 on the one hand, and by this agency combined with stretching on the 
 other, are shown in PI. IX, figs. 1 and 2. The same thing is admi- 
 rably seen in two specimens (Nos. 11651 and 11652) from the Cleveland 
 ore dock in Marquette. (See p. 168.)^ 
 
 If we could desire any more certain proof that these “stretching 
 structures” are of secondary origin, developed in an already solid rock, 
 we should find it in No. 11803 (PI. XIY, fig. 2). Here the porphyritic 
 feldspar crystals lie in the groundmass at every conceivable angle, show - 
 ing that at the time they were formed there was no force to affect their 
 orientation. Their breaking and tearing asunder, however, in every 
 case, has taken place in the direction of the foliation or stretching, 
 without the least reference to the position of the feldspar crystal itself. 
 
 MINERALOGICAL (CHEMICAL) METAMORPHISM OF THE MENOMINEE 
 AND MARQUETTE ROCKS. 
 
 Chemical alteration may go on to almost any extent in massive rocks, 
 unattended by any mechanical deformation ; and yet certain chemical 
 changes in rock-forming minerals seem to be dependent upon the phys* 
 
WILLIAMS.] 
 
 PRODUCTS OF METAMORPHISM. 
 
 209 
 
 ical conditions produced by great orographic strains. It is easy to 
 understand how the crushing of a rock should, as a rule, accelerate 
 chemical activity by increasing the circulation and possibly by raising 
 the temperature by friction ; but more than this, we find that of several 
 different alterations to which a given mineral is subject, certain ones 
 are never found except in those regions where dynamic action has been 
 intense. 
 
 It is true that the same secondary mineral may be produced In differ, 
 ent ways. It may result from the same original mineral under different 
 conditions, or from different minerals under the same conditions, or from 
 different minerals under different conditions. It may also sometimes 
 be derived from a single substance, and sometimes from a reaction be- 
 tween two or more substances. On account of the small number of 
 elements which enter into the composition of rock-forming minerals, 
 their physical differences are due mostly to the different proportions in 
 which these elements are combined. Very slight variation in condi- 
 tions may modify these proportions and so produce one mineral or 
 another. Even in exactly the same chemical compound, what may be 
 a stable state under one set of conditions, may be an unstable state 
 under another set. So delicate is this adjustment that the secondary 
 minerals produced in a given case depend not merely upon the chem- 
 ical composition of the original rock or of its constituents, but even to 
 a greater degree upon the physical conditions obtaining at the time of 
 their formation. Thus with every change of these, one generation of 
 secondary minerals may give place to another. 
 
 Such a succession of alterations, each dependent upon its owmset of 
 conditions, teuds to obscure the life history of a rock mass ; and yct^h^ 
 spite of its complexity, this study is full of promise. It is generally 
 possible to separate the products of metamorphism proper from those 
 of weathering, as described in Chapter I (see p. 36). All the massive 
 rocks of tbe Menominee and Marquette regions offer admirable op- 
 portunity for the study of the first of these alterations, while the more 
 basic types often present the subsequent effects of weathering. 
 
 In reviewing and summing up the results of chemical alteration 
 already described at length, it will be advantageous first to enumerate 
 the minerals of secondary origin, stating briefly the circumstances un- 
 der which each was probably formed, and second to trace out the differ- 
 ent phases of alteration to which each of the more important original 
 constituents has been subjected. 
 
 SECONDARY MINERALS AND THEIR ORIGIN. 
 
 PRODUCTS OF METAMORPIIISM. 
 
 Feldspar . — This mineral is not common as a secondary product ex- 
 cept in the form of albite, which as Lossen has shown (see Chap. I. p. 60) 
 is a very characteristic result of dynamic metamorphism. In the 
 Sturgeon Falls gabbro albite is a common secondary mineral, both as 
 
 Bull. 62 14 
 
210 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [ HULL. 62. 
 
 the base of saussutite and in the form of clear, transparent veins. Here 
 the twinning structure is not frequent, but it may be seen in some of the 
 veins, as is shown in Fig. 4, p. 69. Albite in the form of a fine gran- 
 ular mosaic, with or without quartz also occurs in many of the altered 
 diabases. Its substance is so clear and glassy as to leave no doubt 
 about its being a secondary product. 
 
 Microcline as a secondary mineral is to be referred rather to the effect 
 of pressure twinning than to chemical alteration. 
 
 Saussurite (Chapter I, p. 58) is not a simple mineral, but a mixture 
 derived from the alteration of the lime-soda feldspars. It is abundant 
 in the more basic rocks of the Menominee aud Marquette regions — in 
 the gabbros of Sturgeon Falls and in many diabases and diorites. The 
 base is a clear, soda feldspar (albite) which contains zoisite needles, or 
 more rarely epidote aud colorless garnet. (No. 11189, p. 108.) 
 
 Zoisite occurs only as one of the constituents of saussurite above 
 described. It is in the form of minute needles, without terminations, 
 as shown in Figs. 5 and 6 (pp. 69, 70). These differ much in size, and 
 between crossed nicols display dull bluish interference colors. When 
 the zoisite needles are very small the saussurite is a gray opaque mass, 
 which only the highest power of the microscope is able to resolve. 
 
 Garnet was observed only once, in minute colorless crystals, forming, 
 along with epidote, one of the constituents of the saussurite in speci. 
 men No. 11189. (see p. 108). 
 
 Quartz is a widespread secondary mineral. It often originates from 
 the breaking up of the more acid feldspars, like orthoclase. It may also 
 originate from the lime-soda feldspars. Primary and secondary quartz 
 sometimes present an identical appearance. In some of the Lake Su- 
 perior diabases quartz seems to be an original component, and in others 
 of the more altered ones it is certainly of secondary origin. In a few 
 intermediate cases its origin must always remain doubtful. Owing to 
 the ease with which silica is transported in solution, that which is set 
 free by the decomposition of the silicates is often entirely removed from 
 the rock or is deposited in seams. In at least one instance a brown 
 isotropic substance resembling opal was observed (the gabbro from 
 Eureka Shaft near Marquette p. 170). 
 
 Hornblende . — Although there is reason for considering the hornblende 
 in some of the Menominee and Marquette greenstones as a primary 
 constituent, still there can be no doubt that^this mineral is also the most 
 important secondary component of these rocks. In a fibrous form as 
 uralite, amianth, etc., hornblende is almost the sole representative of 
 the former pyroxene in the more altered and schistose diabases, and the 
 same mineral seems also to be the final metamorphic product of the 
 compact hornblende in the diorites. Indeed, the schistose structure 
 of these rocks is largely due to the production of fibrous hornblende and 
 lamellar minerals of the mica type, and to their arrangement parallel 
 to a single plane. The components of the secondary fibrous hornblende 
 
WILLIAMS.] 
 
 SECONDARY MINERALS. 
 
 211 
 
 are mainly derived from some bisilicate, like pyroxene or compact 
 hornblende, but its position is by no means confined to the area formerly 
 occupied by these substances. On the contrary, the material shows a 
 tendency to wander, and to develop amphibole needles along the cleav- 
 age cracks of the feldspar, as seen in Plate XII, fig. 2. This may even 
 become filled with the hornblende, as in the epidiorite, Xo. 11663, from 
 Pine street, Marquette, and the whole rock be finally reduced to a fine, 
 felt-like mass, as shown in Plate IX, fig. 1. 
 
 Compact hornblende also, both brown and green, appears to have re- 
 sulted extensively in the greenstones from the direct alteration or 
 molecular rearrangement of pyroxene. Such a change has often been 
 recorded, as stated in Chap. I. Indeed, the probability that much of 
 the pyroxene of the original rocks has passed into fibrous green horn- 
 blende through an intermediate stage of compact hornblende has already 
 been alluded to (p. 72). The brown or basaltic variety is to be found 
 associated with the diallage of the Sturgeon Palls gabbro, as shown in 
 PI. VIII, figs. 1 and 2; also in the porphyritic rock from the western 
 end of the u gabbro ridge,” near Little Quinnesec Falls, on the Meno- 
 minee. The compact green hornblende of Xos. 11176 and 11178, from 
 the Four-Foot Fall, and of many of the Horse Race diorites, has pre- 
 cisely the form of diabasic augite ; and in spite of its compact structure 
 shows in its pale color and darker green border clear evidence of its 
 secondary origin. 1 The pale compact hornblende of the barrier rock 
 at Upper Quinnesec Falls (Xo. 11054) looks exactly like diallage, 2 and 
 under the microscope its most exceptional orthopinacoidal parting 
 bears testimony to its derivation from this mineral. (See p. 103.) 
 
 The manner in which the compact hornblende ravels out and becomes 
 fibrous is often clearly seen in the Lake Superior greenstones, and is 
 shown in PI. XII, fig. 1, and in Fig. 19 on p. 126. 
 
 Epidote is a common metamorphic mineral, and appears almost al- 
 ways in small but well formed yellowish crystals. It sometimes forms 
 one of the constituents of saussurite, but far less frequently than zoisite, 
 as more iron is necessary for its genesis. In one case, Xo. 11091, the 
 feldspar of a coarsely granular. rock from the Horse Race, seems wholly 
 changed to large individuals of epidote, while the pyroxene has given 
 place to corresponding areas of a rather compact greenish hornblende (p. 
 108). In Xo. 11712, from the Brook Section, near Marquette, the change 
 of the feldspar to epidote is less complete. Epidote more commonly 
 results from the alteration (perhaps weathering) of some ferrous bisili- 
 cate. Here it is generally in association with bright green chlorite in 
 the form of the characteristic aggregate described in Chap. I (p. 56). 
 This is very common in many of the more altered greenstones of the 
 regions studied. (See PI. XI, fig 1.) 
 
 1 See PI. XII, fig. 2; and cf. Loasou : Erliiut. zur. geol. Spe.cialkarto von Preuaaen, Platt Ilarz- 
 gerode, 1882, p. 81; and William a’ Bull. U. S. Geol. Survey, No. 28, PI. I, fig. 2; PI. H, fig. 1,1886. 
 
 2 cf. H. Credner: Neues Jahrbuch fur Mineral., 1870, p. 972. 
 
212 GREENSTONE SCHIST AREAS OF MICHIGAN. [bull. 62. 
 
 Biotite originates under certain -circumstances from hornblende. This 
 is an alteration well known to mineralogists, 1 and may be admirably 
 seen in several of the Horse Race diorites and in the curious amphi- 
 bole granite, No. 11831, figured in PI. XYJ, fig. 2. 
 
 Muscovite , Sericite . — The potash micas hold a similar place in relation 
 to orthoclase, as a product of dynamic metamorphism, that saussurite 
 does to the lime^soda feldspars. In some specimens, as for instance in 
 the granite No. 11089 from the Horse Race and in No. 11660 from the 
 so-called gold mine near Pine street, Marquette, broad plates of typical 
 muscovite are developed in the feldspar ; generally, however, the alter- 
 ation is due to the minute scales or curved foliie called sericite. These 
 two minerals are quite identical in composition and generally in origin, 
 as has been explained in Chap. I. The development of sericite may be 
 best studied in the schistose porphyries, which owe their cleavage to 
 stretching. These are abundant in both the regions investigated, 
 especially at Upper Quinnesec Palls (see Chap. Ill, and PI. XIY, fig. 
 3) and near the city of Marquette (Chap. IY). While the production 
 of sericite in the acid rocks is for the most part the result of intense 
 dynamic action, it would seem as though it were especially liable to re^ 
 suit, like certain varieties of chlorite (see below), when this force acted 
 as a tension rather than as a compression. 
 
 Titanium minerals . — The metamorphosed eruptive rocks of the re- 
 gions studied offer unusual opportunities for tracing the varied trans- 
 formations of the titanium compounds. It is doubtful whether this 
 element existed in the original rocks in any other form than titanic iron 
 (ilmenite) or as a component of certain biotites. In the metamorphic 
 rocks, however, titanium minerals are numerous and their origin can 
 be traced to different sources. The probable derivation of rutile and 
 magnetite from ilmenite may be seen in No. 11070, from Upper Quin- 
 nesec Palls (PI XIII, fig. 2), and also in No. 11825, from northwest of 
 Marquette (p. 181). The little “ Thonscliiefernadeln,” shown in Fig. 12 
 (p. 106), seem also to have been derived from ilmenites. A sagenitic 
 network of rutile produced by the alteration of biotite and the conse- 
 quent freeing of titanic oxide is seen in No. 1111 3, from Iron Mountain; 
 in No. 11672 from Marquette; and in No. 11738, from near Baldwin’s 
 Kilns, Negaunee. 
 
 Anatase, along with leucoxene, has resulted from the alteration of 
 ilmenite in No. 11130, from Twin Falls (Fig. 26$ p. 166) and in No. 
 11802, north of Negaunee, near the Carp River. Anatase seems also 
 to have resulted from the decompositon of titaniferous biotite in Nos. 
 11050 and 11052, from near Upper Quinnesec Falls. 
 
 Sphene in the form of leucoxene is a universal result of the alteration 
 of ilmenite in the metamorphosed diabases. In rare cases, like No. 
 11014, from Lower Quinnesec Falls, it is intimately associated with 
 
 *See J. Roth: Allgomeine undcheimsche Geologie, vol. 1, p.333, 1879, and Inostrauzeff : Metamor- 
 phosirte Gesteine im Gouvernment Olonez, 1879, p. 192. 
 
WILLIAMS J 
 
 PRODUCTS OF WEATHERING. 
 
 213 
 
 rutile, which may have been produced simultaneously with the altera- 
 tion of the leucoxene, or have resulted from it. In other exceptional 
 cases the product of the ilmenite appears with all the crystal form and 
 physical properties of rock-forming sphene. Such an occurrence in No. 
 11189 from the Horse Race is shown in PI. XIII, fig. 1 ; and another 
 in No. 11831, from northwest of Marquette, in PI. XVI, fig. 2. 
 
 The secondary minerals thus far enumerated are products of meta- 
 morphism proper, as distinguished from weathering j that is, they are 
 highly crystalline, and have been produced under circumstances very 
 different from those ordinarily prevailing at the earth’s surface. Here 
 the tendency is for the more crystalline and less soluble compounds to 
 become more soluble through union with water and carbon dioxide. 
 Hydration and carbonatization are therefore characteristic results of 
 surface action upon rocks. They bring about their disintegration and 
 decay, as purely metamorphic processes do not. Both metamorphism 
 and weathering are very apparent in the eruptive masses of the Me- 
 nominee and Marquette regions. The rocks of Keweenaw Point, on 
 the other hand, show only the effects of weathering. In spite of their 
 great antiquity they have not undergone metamorphism in the strict 
 sense. Much younger rocks in disturbed areas are often found to be 
 intensely metamorphosed, which clearly shows that something besides 
 mere lapse of time is necessary to accomplish this change. 1 
 
 PRODUCTS OF WEATHERING. 
 
 The secondary minerals in the Menominee and Marquette massive 
 rocks which owe their existence to atmospheric action or weathering 
 belong mainly to the following species: Chlorite, talc, serpentine, car- 
 bonates (calcite, dolomite, etc.), iron-hydroxide, and pyrite. 
 
 (Jlilorite is generally a product of weathering, but its origin is some- 
 times closely associated with dynamic agencies. For instance, it is a 
 constant feature in the basic rocks which have been stretched (like se- 
 ricite in the more acid ones), filling with its parallel folia the interstices 
 between the broken and separated fragments, and thus imparting a 
 degree of schistosity to the entire mass, (see PI. XT, fig. 2.) The 
 ordinary process of chloritization has been described in Chapter I, and 
 frequently alluded to in the petrographical descriptions, since it is ex- 
 tremely common in the basic eruptives. If the original mineral was very 
 poor in iron an almost colorless chlorite was the result, as in the Stur- 
 geon Falls gabbro (PI. VIII, fig. 2). In the highly ferruginous dia- 
 bases, on the other hand, the chlorite has a deep green color and is 
 often pleochroic. This is the li viridite” of the older authors, which is 
 
 1 Tho efficiency of orographic movements to bring about this result lias already been sufficiently 
 emphasized. The observations of Losson that similar changes may be produced by the contact action 
 of large masses of intrusive granite have been briefly referred to in Chapter I. To what extent the 
 enormous granite areas lying on both sides of the Marquette and Menominee greenstone bolts may 
 havo been instrumental in effecting their miueralogical metamorphism must for tho present bo left 
 undecided, inasmuch as no evidence directly bearing upon this question has as yet been collected. 
 
214 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [BULL. 62. 
 
 frequently associated with sharply defined epidote (secondary augite of 
 Wichmann), as figured in PL XI, fig. 1. Chlorite seems to be the 
 common effect of weathering upon pyroxene, hornblende, and biotite. 
 
 The peculiar variety of chlorite known as “ helminth” in vermiform 
 aggregates occurs imbedded in secondary quartz in some of the Stur- 
 geon Falls gabbros, and is represented in Fig. 8 on p. 71. 
 
 Talc results in some cases from the alteration of hornblende, as ob- 
 served by Tschermak, 1 Inostranzeff, 2 Becke, 3 and the writer. 4 This is 
 not a common phenomenon in the Michigan greenstones, but some ad- 
 mirable examples were observed in the coarse grained diorites of the 
 Horse Bace above Upper Quinnesec Falls. 
 
 Serpentine . — The scarcity of olivine in the rocks examined makes the 
 ordinary derivation of serpentine uncommon. This, however, does oc- 
 cur in some of the least altered diabases of Marquette. Indeed, ser- 
 pen tinization is almost the only effect of weathering noticeable in some 
 specimens from the great dike of Lighthouse Point (olivine diabase), 
 certain weakly polarizing fibers resulting from the change of hornblende 
 appear to be serpentine, which, according to Eosenbusch, 5 frequently 
 gives rise to this mineral. An instance of this may be seen in Nos. 
 11078 and 11191 from the Horse Race (p. 109). 
 
 Carbonates . — These most frequent products of weathering abound in 
 the most altered greenstones, but they are nevertheless not unfrequently 
 absent on account of the readiness with which these compounds are 
 removed in solution. Calcite and dolomite are not microscopically dis- 
 tinguishable without a chemical reaction, but this is hardly necessary 
 for most cases. 
 
 Iron-hydroxide and Pyrite are both iron compounds universally pro- 
 duced in basic rocks under ordinary atmospheric influences. The Mich- 
 igan greenstones present no exception in the amount of these minerals 
 which they contain. 
 
 PROGRESS OP ALTERATION IN THE ORIGINAL MINERALS. 
 
 Feldspar gives alteration products depending very largely upon its 
 original composition, whether alkaline or calciferous. By far the most 
 common change in the more basic rocks is to saussurite. This varies in 
 different cases from a comparatively coarse grained zoisite aggregate to 
 a dull gray, almost opaque mass which, even in the thinnest sections, 
 is beyond the highest power of the microscope completely to resolve. 
 The saussuritization may be often seen to have proceeded from the 
 periphery of the feldspar crystal inward. In such cases a compara- 
 tively unaltered center remains, as in No. 11168 from Sturgeon Falls 
 (PI. VIII, fig. 2). Quite as frequent is the occurrence of a clear per- 
 
 1 Tschermak’s mineral, u. petrog. Mittheil., vol. 4, p. 65, 1876. 
 
 2 Metamorpliosirte Gesteine im Gouvemment Olonez, Leipzig, 1879, p.’ 167. 
 
 3 Tschennak’s mineral, u. petrog. Mittheil., vol. 4, 1882, pp. 339 and 349. 
 
 4 Bull. IT. S. Geol. Survey, No. 28, p. 58, 1886. 
 
 6 Mikroa. Physiog., 2d ed., vol. 2, p. 108. 
 
Williams. ] 
 
 ALTERATION PRODUCTS OF FELDSPAR. 
 
 2 15 
 
 ipliery around, feldspar crystals which have been completely saussuri- 
 tized. (See No. 11167 from Sturgeon Falls (PI. VIII, fig. 1 ); No. 
 11054 from Upper Quinnesec Falls, and No. 11182 from the Horse Eace.) 
 The clear feldspar substance in such cases appears like a new crystalli- 
 zation rather than an unaltered survival of the original individual (cf. 
 Fig. 4, p. 69). 
 
 The inverse ratio existing between the mechanical and the chemical 
 action visible in the altered feldspars of the basic rocks has been often 
 alluded to on pp. 88, 169. This seems to be the reverse of what might 
 be expected, as well as of what is actually observed in the case of all 
 the other constituents. It is, however, frequently the fact that, in a 
 continuous rock mass, feldspar is most completely saussuritized which 
 occurs in the least crushed portion, while the rock which is most broken, 
 stretched, and foliated retains its feldspar fragments in a quite fresh 
 and unaltered condition. That this fresh feldspar is not a new crys- 
 tallization, is proved by the fact that fragments can often be seen to 
 have once fitted together, as portions of one individual, before the 
 crushing took place. Among many sections in which this phenomenon 
 can be observed may be mentioned : The Sturgeon Falls gabbro; the 
 rocks of the diorite ridge near the Lower Quinnesec Falls ; Nos. 11004, 
 11010,11019, afid 11102 from just below the Lower Quinnesec Falls ; 
 Nos. 11054, 11073, and 11056 (see Fig. 11) from Upper Quinnesec Falls; 
 No. 11179 from Four-Foot Falls, and Nos. 11651 and 11652 from the 
 Cleveland ore dock in Marquette. 
 
 Such observations, made at many widely separated localities within 
 the Menominee and Marquette greenstone areas, would at first thought 
 seem to indicate that there is a reciprocal relation between the chemical 
 and mechanical effects produced by great pressure. In other words, 
 that the force which in the m assive portion of the rock caused increased 
 chemical action and alteration of the feldspar to saussurite, was ex- 
 pended, in another part, in the work of crushing. The fact, however, 
 that the bisilicate constituents are more altered in the crushed bands 
 than in the Other part of the rockmass is opposed to such an explana- 
 tion, and seems rather to indicate that the more ready alteration of 
 these and the production of such minerals as fibrous hornblende, chlorite, 
 and talc, formed a soft matrix which protected the feldspar from the 
 further action of pressure and chemical action. 
 
 A totally different alteration from saussuritization is sometimes ob- 
 served in the feldspars of the more basic eruptives. This consists of 
 their change to green hornblende needles, and can of course occur only 
 where a portion of the necessary elements is furnished by some bisili- 
 cate. These elements (i. e., magnesium and iron) wander along the 
 cleavage cracks of the feldspar, causing the development of the needles 
 as shown in PI. XU, fig. 2. A very complete instance of this change 
 is shown in the epidiorite, No. 11663, from Pine street, Marquette. 
 
 Still another alteration of the plagioclase is to epidote. This is com- 
 
216 
 
 GREENSTONE SCHIST AREAS OF MICHIGAN. 
 
 [HULL.. 62 . 
 
 plete in No. 11091 from the Horse Race, and partial in No. 11712 from 
 the Brook Section, near Marquette. 
 
 While the lime feldspars change to zoisite, epidote, or hornblende, the 
 alkaline feldspars show a corresponding tendency to pass into mica 
 (sericite). This process is most commonly central, the periphery of a 
 crystal remaining intact after the interior is completely altered, as may 
 be seen in No. 11104, the granite from south of Upper Quinnesec Falls. 
 This same specimen exhibits an interesting phase of the inverse ratio 
 existing between the mechanical and the chemical action in the acid 
 feldspar. Micro dine seems to have been abundantly developed from 
 orthoclase by pressure but while the orthoelase itself is sericitized, the 
 microcline never shows a trace of this change. 
 
 Pyroxene is comparatively rare in the rocks studied, occurring only 
 as diallage in the Sturgeon Falls gabbro, and as augite in the younger 
 Marquette diabases $ nevertheless, from the structure of many of the 
 other rocks, we may affirm with certainty that they once contained py- 
 roxene, and may hence trace the alterations which this mineral has un- 
 dergone. 
 
 The most common, and indeed the almost universal change of the 
 pyroxene in the Menominee and Marquette rocks is to hornblende. The 
 compact brown hornblende in the Sturgeon Falls gabbro and in the 
 porphyritic rocks from the west end of the ridge near Lower Quinnesec 
 Falls, shows strong evidence of having originated from pyroxene, but 
 this can not perhaps be regarded as beyond all doubt. Compact green 
 hornblende appears to replace original diallage in the gabbro-like 
 diorite which forms the barrier rock at Upper Quinnesec Falls (see 
 PI. X, fig. 1), where it even retains the orthopinacoidal parting. The 
 same mineral likewise seems to replace original augite in many of the 
 Horse Race diorites, whose structure is typically diabasic. " 
 
 Fibrous green hornblende or uralite is too common and well known 
 an alteration product of pyroxene to deserve especial description. It 
 is universally distributed through all of the more basic rocks in the 
 areas investigated. 
 
 A colorless chlorite may be seen originating from the almost color- 
 less diallage of the Sturgeon Falls gabbro, as shown in PI. VIII, fig. 
 2. From the varieties of pyroxene which are richer in iron, a deep green 
 chlorite results which is often associated with epidote, as shown in PI. 
 XI, fig. 1. 
 
 Hornblende . — Without reference to the original or secondary origin of 
 the hornblende itself, this mineral is found subject to several different 
 alterations. 
 
 It passes from the compact to the fibrous form by fraying out at the 
 ends, as shown in specimen No. 11175, from the Four-Foot Fall (see 
 Fig. 19, p. 126). It also seems to give rise to biotite in many of the 
 Horse Race diorites and in the amphibole granite, No. 11831, obtained 
 at the camp northwest of Marquette. (See PI. XVI. fig. 2.) Talc 
 
williams.] BIOTITE, OLIVINE, AND ILMENITE. 217 
 
 frequently is produced by hornblende alteration in the Horse Race 
 diorites as described in Chap. Ill (p. 107). A colorless chlorite, closely 
 resembling that produced from the Sturgeon Falls diallage, is derived 
 from the pale hornblende (itself probably paramorphic) of No. 11098, 
 from the ridge near Lower Quinnesec Falls. This is produced in spots 
 over the hornblende and is visible only by its isotropic behavior in polar- 
 ized light, as shown in Fig. 9 (p. 79). The viridite (chlorite) epidote 
 aggregate originates from hornblende just as it does from pyroxene. 
 Finally serpentine is an exceptional result of hornblende alteration, as 
 may be seen in specimens 11078 and 11191 from the Horse Race (p. 109). 
 
 Biotite shows the usual alterations and is principally the result 
 of weathering rather than of metamorphic processes. Bleaching first 
 takes place and then chloritization. Carbonates are sometimes sepa- 
 rated in the form of interpolated lenses, while the titanium which 
 entered into their composition separates out sometimes as anatase 
 (Nos. 11050 and 11052 from Upper Quinnesec Falls) and sometimes as 
 rutile. 1 (Nos. 11113, from near Iron Mountain in the Menominee valley, 
 No. 11672 from Marquette and No. 11738 from the Brook Section.) 
 
 Olivine occurs only in a few of the Marquette diabases, where its 
 alteration is the usual one to serpentine. 
 
 . Ilmenite is the last of the important original constituents of the 
 Menominee and Marquette massive rocks whose alterations can be 
 clearly traced. This gives rise to a variety of new titanium minerals 
 
 Its commonest change is that to leucoxene, which is everywhere 
 encountered, see PI. IX, figs. 1 and 2. 
 
 Sphene or titanite, of which leucoxene is only a special form, some- 
 times originates from ilmenite, as is shown in PI. XIII, fig. 1, and in 
 PL XVI, fig. 2. 
 
 Anatase also, in association with leucoxene, is a secondary product 
 of ilmenite alteration. This is shown in Fig. 25 (p. 131) of No. 11130, 
 from Twin Falls, as well as in No. 11802, one of the stretched agglom- 
 erates on the Carp River. (See Chap. Y, p. 177.) 
 
 'On the frequency of these changes see Whitman Cross: “ Petrography of the Leadville Kocks” 
 in Mon. U. S. Geol. Survey, vol. 12, 1887. 
 
PLATES. 
 
PLATE VIII. 
 
PLATE VIII. 
 
 Fig. 1. — Saussurite gabbro ( first stage). 
 
 From point h, PI. Ill, at Sturgeon Falls, Menominee River, Michigan. Specimen 
 No. 11167a. Ordinary light. (See p. 68.) 
 
 The triclinic feldspar, which shows occasional idiomorphic forms indicating that 
 it is in part, at least, older than the pyroxene, here appears almost completely altered 
 to an opaque, gray saussurite. A high magnifying power resolves this into an aggre- 
 gate of minute zoisite needles, calcite and albite. These are somewhat unevenly dis, 
 tributed which produces the blotched appearance of the saussurite. , 
 
 The diallage, which is of a pale green color in the hand-specimen, is almost color- 
 less when seen under the microscope. Its well marked orthopinacoidal parting is seen 
 on the right of the figure. This diallage is surrounded by a border of compact horn- 
 blende, which is either brown, pale green or colorless. It frequently becomes fibrous 
 on’ its exterior edge, as is shown in Fig. 7, on p. 70. Small patches of compact brown 
 hornblende are also abundantly scattered over the entire surface of the diallage in a 
 manner that would seem to indicate that it had originated from the latter by para- 
 morphism. There is some pale green chlorite visible in the upper part of the draw- 
 ing and on the right is a bit of ilmenite and leucoxene. 
 
 Fig. 2. — Saussurite gabbro ( second stage). 
 
 From point /, PI. Ill, at Sturgeon Falls, Menominee River, Michigan. Specimen 
 No. 11154. Represented between crossed nicol prisms. (Seep. 72.) 
 
 A large individual of the pale diallage is here seen in an advanced stage of altera- 
 tion to a colorless chlorite. Because of the almost isotropic character of this mineral, 
 it is necessary to show its appearance in polarized light. Imbedded in the chlorite 
 are remnants of the still brightly polarizing diallage, and around it is the border of 
 hornblende, which here shows pale yellow interference colors. 
 
 The feldspar is less completely saussuritized than in the last figure. Its character- 
 istic twinning lamellae are still visible in many instances, particularly at the center 
 of the crystals. 
 
 222 
 
U.S. GEOLOGICAL SURVEY 
 
 BULLETIN No. 62 PLATE VIII. 
 
 FIG. 2 ( X30) 
 
 G H.W DEL 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
PLATE IX. 
 
 223 
 
PLATE IX. 
 
 Fig. 1 . — Altered diabase or diorite. 
 
 From the so-called u Gabbro Ridge, ” below Lower Quinnesec Falls, Menominee River, 
 Michigan. Specimen No. 11028. Ordinary light. (Seep. 81. ) 
 
 The original structure of this rock has been completely changed, in spite of its still 
 massive character. It is now composed of pale green, fibrous hornblende, saussurite, 
 quartz, calcite, chlorite, ilmenite, and leucoxene. Most of these constituents are of 
 secondary origin, and in the process of their formation the form of the primitive min- 
 erals has been so completely obliterated that it is now impossible to say whether the 
 mother-rock was a diabase or a diorite. 
 
 Fig. 2. — Schistose band in the last figured rock, showing the effect of dynamic metamor- 
 phism ( stretching ) upon it. 
 
 Locality same as that of last figure. Specimen No. 11031. Ordinary light. (See 
 
 p. 82.) 
 
 The feldspar in this rock is chemically less altered than in the last, but it has been 
 subjected to a much more intense mechanical action. It is fractured, aud the frag- 
 ments are widely separated, although those pieces which once belonged to the same 
 crystal may still often be identified. The interstices are filled with scales of a green 
 chlorite, arranged parallel to one another, so as to produce a schistose structure. 
 Even the little leucoxene zones around the ilmenite grains have been elongated in 
 the same direction. 
 
 224 
 
U.S. GEOLOGICAL SURVEY. 
 
 BULLETIN No 62 PLATE IX. 
 
 G.hw del 
 
 FI G.2 ( XOO ) 
 
 FlG.l (X80) 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILUHOIS 
 
PLATE X 
 
 Bull. 62 15 
 
 225 
 
PLATE X. 
 
 Fig. 1 . — Saussurite diorite. 
 
 This rock forms the barrier at Upper Quinnesec Falls, Menominee River, Michigan. « 
 Specimen No. 11054. Ordinary light. (See p. 103.) 
 
 In spite of the close external resemblance of this rock to the Sturgeon Falls saus- I 
 surite gabbro (PI. VIII, fig. 1), it shows no trace of any pyroxenic constituent. Its ; 
 only bisilicate is hornblende. This is sometimes compact (and then both brown and 
 green in color), sometimes ragged and fibrous. The former variety is seen in the 
 center and on the left of the figure, with its remarkably perfect orthopinacoidal t 
 parting, like that recently observed by Cathrein in a hornblende from Roda, in the 
 Tyrol. This parting may be an indication that this hornblende has been derived 
 * from original diallage. A large individual of the more ragged and fibrous hornblende, 
 filled with secondary quartz, is shown on the right of the figure. 
 
 The feldspar of this rock has undergone the usual alteration to opaque, gray saus- 
 surite, but in this are imbedded frequent grains of a fresh brown feldspar. Leu- . 
 coxene rims around the ilmenite are abundant. 
 
 Fig. 2 . — Typical aphanitic greenstone of the Marquette region. 
 
 From Baldwin’s Kilns, northeast of Negaunee, Michigan. Specimen No. 11747. Or- 
 dinary light. (See p. 172.) 
 
 This is a fair representative of the commonest rock type in the southern Marquette 
 and Negaunee greenstone areas. Its grain must always have been very fine and com- 
 pact. Long, slender feldspar crystals may still be seen, sometimes with an imper- 
 fectly developed form, such as is common in the semi-crystalline rocks (porphy rites), i 
 The groundmass is composed of a fine grained aggregate of fibrous hornblende, 
 chlorite, quartz, calcite, and ilmenite leucoxene. These minerals are all secondary, 
 and may easily have resulted from the alteration of a cryptocrystalline, or even a 
 partially vitreous base. 
 
 226 
 
U.S. GEOLOGICAL SURVEY 
 
 BULLETIN No. 62 PLATE X. 
 
 FTG.I ( X30) 
 
 FI G. 2 ! X I IO ) 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
PLATE XI. 
 
PLATE XI. 
 
 Fig. 1 .-Chlorite-epidoie aggregate in an altered diabase. 
 
 From below Upper Quinnesec Falls, Menominee River, Michigan. Specimen No. 
 
 11049. Ordinary light. (See p. 97.) 
 
 This is a very common alteration product in rocks of the diabase type, especially 
 in those rich in iron. In a confused mass of deep green and somewhat pleochroic* 
 chlorite scales lie embedded extremely sharp crystals of a yellowish or colorless 
 epidote. These latter are what the earlier students of these rocks mistook for! 
 secondary augite. In the lower part of the figure are seen ilmenite grains sur- 
 rounded by rims of leucoxene and a portion of a large secondary hornblende crystal.) 
 
 Fig. 2 . — Stretched greenstone. 
 
 From above Lower Quinnesec Falls, Menominee River, Michigan. Specimen No. 
 
 11102. Ordinary light. (Seep. 94.) 
 
 The effects of tension upon a solid rock mass are rarely seen more distinctly than 
 in this specimen. Not only the feldspar, but also a large grain of ilmenite has here 
 been forcibly torn asunder, and the fragments have been separated a considerable dis- 
 tance, always in one direction. The peculiar green chlorite so characteristic of all 
 stretched basic rocks (cf. PI. IX, fig. 2) fills the interstices between the mineral frag- 
 ments. It must have crystallized after the breaking of the solid rock constituents 
 and its scales, which are all arranged parallel to the direction in which the strain 
 was exerted, produce a decidedly schistose structure in the rock. The fresh state oi 
 the feldspar in a rock which has been subjected to such intense mechanical action as 
 this one is very noticeable. 
 
 228 
 
U S. GEOLOGICAL SURVEY. 
 
 BULLETIN No. 62 PLATE XI 
 
 PIG. I ( X 180 ) 
 
 FIG 2 1X30) 
 
 H.W DEL . 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
PLATE XII 
 
PLATE XII. 
 
 Fig. 1 . — Coarsely crystalline diorite. 
 
 From near Baldwin's Kilns, northeast of Negaunee, Michigan. Specimen No. 11749. 
 
 Ordinary light. (See p. 173.) 
 
 This one of the coarse grained dike rocks which penetrate the aphanitic green- 
 stones of the Negaunee area. The hornblende is idiomorphic, and, as there are no 
 certain traces of pyroxene, the rock is designated a “ diorite.” The feldspar is 
 quite filled with secondary actinolite or epidote needles. The hornblende is often 
 altered internally to chlorite or fibrous amphibole, while its exterior still remains 
 compact and shows a curious concentration of the green coloring matter. There is 
 also observable around the edge of the hornblende crystals a separation into fibers, 
 as described by Becke. 
 
 Fig. 2. — Epidiorite. 
 
 From the Horse Race above Upper Quinnesec Falls, Menominee River, Michigan. 
 
 Specimen No. 11186. Ordinary light. (See p. 107.) 
 
 This is one of the coarse grained dioritic rocks so abundant along the Horse Race 
 Rapid. The pale green hornblende is entirely allotriomorphic and fills the spaces 
 between the idiomorphic feldspar crystals exactly as augite does in diabase. Still 
 there is no certain trace of pyroxene now present. The hornblende shows a deeper 
 color around its edge aDd a breaking up into fibers, which are arranged in irregular 
 bundles and appear to wander off into the surrounding feldspar. 
 
 230 
 
U.S. GEO LOG I CAL SURVEY. 
 
 BULLETIN No. 62 PLATE XII 
 
 FIG. I ( X I IO ) 
 
 FIG. 2 IXIIOI 
 
 G.H.W DEL . 
 
IHt LIBRARY 
 Of THE 
 
 UNIVERSITY OF ILUWIS 
 
PLATE XIII. 
 
PLATE XIII. 
 
 Fig. 1. — Sphene crystals around ilmenite. 
 
 In a dioritic rock from the Horse Race Eapid, above Upper Quinnesec Falls, Meno- 
 minee River, Michigan. Specimen No. 11189. Ordinary light. (See p. 109.) 
 These sphene crystals, although their minerological character is undoubted, are 
 not so clear or so sharply defined as usual. They are gray and cloudy, resembling 
 leucoxene in appearance; and, like this substance which is known to be identical 
 .with sphene in its composition, these crystals surround grains of iimenite, as though 
 they had originated from its alteration. If this be the case, we have here an inter- 
 esting example of leucoxene assuming its characteristic titanite form. 
 
 Fig. 2. — Rutile originating from the alteration of ilmenite. 
 
 In a greenstone from below the Upper Quinnesec Falls, Menominee River, Michigan. 
 Specimen No. 11070. Ordinary light. (See p. 99.) 
 
 The rock, which was probable once a diabase, now consists principally of green 
 chlorite and reddish feldspar substance. The opaque iron oxide now present is 
 magnetite. This occupies irregular areas and is intimately associated with a net- 
 work of yellow rutile needles in a manner which renders probable the origin of both 
 of these minerals from an original ilmenite. 
 
 232 
 
U. S. GEOLOGICAL SURVEY 
 
 BULLETIN No 62 PLATE XIII. 
 
 FIG. I (XQO) 
 
 FIG 2 IXIIOI 
 
 G H W DEL 
 
THE LIBRARY 
 OF THE 
 
PLATE XI Y 
 
PLATE XIV. 
 
 Fig. 1 . — Sericite porphyry. 
 
 From just below the Upper Quinnesec Falls, Menominee River, Wisconsin. Specimen 
 No. 11050. Nicols crossed. (Seep. 121.) 
 
 This rock, which was once an eruptive quartz porphyry, shows in an admirable 
 manner the effect of stretching. The porphyritic quartz crystals are somewhat 
 elongated and testify to the tension to which they have been subjected by an undu- 
 latory extinction. The porphyritic feldspar crystals are fractured and pulled apart 
 always in the same direction, without reference to the position which they thern- 
 selwes occupied in the rock. The fissures are cemented by a new crystallization of 
 sericite. The microgranitic groundmass has been rendered schistose by stretching and 
 by the abundant production of sericite, whose scales have a parallel arrangement. 
 
 Fig. 2 . — Stretched and hrecciated greenstone. 
 
 From near the Carp River, north of Teal Lake, Michigan. Specimen 11803. Nicols 
 
 crossed. (Seep. 177.) 
 
 Some of the interstitial material, occurring between the massive cores of the 
 spheroidally parted (hrecciated) greenstones, contains distinct crystals of white 
 feldspar. Between the eastern end of Teal Lake and the Carp River some of these 
 massive cores are themselves much elongated by stretching. (See Fig. 27, p.177.) A 
 section of the insterstitial material from this locality was selected for illustration be- 
 cause of the distinctness Avith which this stretching is apparent in the feldspar 
 crystals. They are always broken and pulled apart in the same direction, while the 
 smaller components of the rock show a corresponding elongation. The continuity of 
 the original rock-structure in the interstitial portion of this exposure indicates that 
 the spheroidal parting is in this case a result of cooling, rather than of mechanical 
 brecciation in situ. (See p. 167.) 
 
 234 
 
U.S. GEOLOGICAL SURVEY. 
 
 BULLETIN No. 62 PLATE XIV. 
 
 FIG. I (X30) 
 
 FIG. 2 ( X30) 
 
 G. H.W DEI. 
 
the UBRMK 
 Of THE 
 
 USIVERSITY OF ILUIOB 
 
PLATE XV. 
 
PLATE XV. 
 
 Fig. 1. — Structure of one of the 11 Augen” in an “Augengneiss,” or stretched granite por- 
 
 phyry. 
 
 From a schistose dike in the greenstones of the Horse Race Rapid above Upper Quin- 
 nesec Falls, Menominee River, Michigan. Specimen No. 11184. Ordinary light. 
 (Seep. 118.) 
 
 The center of the “Auge,” or eye, is seen to consist of a portion of an old, brown 
 colored porphyritic feldspar crystal. This is granulated on either side, and pulled 
 out into a lens, whose longest axis agrees with the direction of the foliation. The 
 granulation is composed of a new crystallization of the feldspar substance, which is 
 clear, and although granitic in structure, it has a much coarser grain than the rest 
 of the rock. This formation of an “Auge” out of a porphyritic feldspar crystal 
 agrpes with the observations of J. Lehmann, Chelius, and others. 
 
 Fig. 2. — Stretched quartz porphyry . 
 
 From a conformable dike in the schistose greenstones of the Brook Section, west of 
 Marquette, Mich. Specimen No. 11707. Nicols crossed. (Seep. 150.) 
 
 This rock is particularly noticeable on account of the wonderful manner in which 
 it shows the effects of a stretching action upon quartz. The original crystals are 
 elongated into lenticular and pear shaped forms, or even into long, narrow bands. 
 The first effect of the tension is to disturb the optical homogeneity and produce an 
 undulatory extinction. If, however, the strain is great enough to overcome the force 
 of cohesion, a mosaic of interlocking and differently orientated grains is the result. 
 Similar phenomena have been observed and illustrated by J. Lehmann in Saxony. 
 The porphyritic feldspar crystals in this rock are. not broken, nor do they show the 
 evidence of great pressure. Their form is generally intact, but it is worthy of re- 
 mark that their center is always occupied by an irregular area of microcline. 
 
 The groundmass is finely microgranitic, containing sinuous bands of micaceous 
 minerals, which bend around the porphyritic constituents, while they follow the 
 general direction of the foliation. 
 
 236 
 
U S. GEOLOGICAL SURVEY. 
 
 BULLETIN No. 62 PLATE XV. 
 
 FIG. I ( X30) 
 
 FIG. 2 ( X30) 
 
 H.W DEL 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
PLATE XVI. 
 
 237 
 
PLATE XVI. 
 
 Fig. 1. — Greenstone schist (tuff) of the northern Marquette area. 
 
 Lighthouse Point, Marquette, Mich. Specimen No. 11619. Ordinary light. (See 
 p. 155.) 
 
 A characteristic, although by no means universal structure, in the banded green 
 schists which compose so large a portion of the region around Marquette, consists in 
 the tufted form of the hornblende crystals. These, although quite compact at their 
 centers, are fibrous at the ends and expand so as to resemble sheaves tied in the mid- 
 dle. The fibers are so fine and the radial arrangement at the ends of the bundles is 
 so perfect that the arm of a black cross is seen to sweep across the field when the 
 thin section is viewed between crossed nicol-prisms. Hornblende with a structure 
 like this has been observed by Renard and others" as a new crystallization in altered 
 sediments, a fact which lends additional support to the hypothesis that these green 
 schists are tuff deposits. 
 
 # 
 
 Fig. 2. — Amphibole granite (?) forming a dike in aplianitic greenstones. 
 
 Northeast of Negaunee, Mich. Specimen No. 11831. Ordinary light in part ; polar- 
 ized light in part. (See p. 181.) 
 
 This rock presents many points of interest, both in its structure and alteration 
 products. The feldspar is in two distinct generations, of which the older variety is 
 entirely idiomorphic, with a zone of clear substance surrounding a gray and more 
 altered interior. 
 
 The hornblende exhibits the unusual alteration to biotite, which is sometimes 
 brown, sometimes green. This mineral in rare instances has crystallized in sharp 
 hexagonal plates which show pressure lines of cleavage (“ Drucklinien ”). 
 
 The groundmass of this rock is an aggregate of quartz and the younger generation 
 of feldspar. These sometimes form a microgranitic mosaic and sometimes micro- 
 pegmatitic growths, which are represented in the figure as they appear in polarized 
 light. Apatite is abundant, and also ilmenite or magnetite surrounded by chlorite, 
 and in some cases by sphene, as though this had resulted from the alteration of tfie 
 ilmenite, as shown in PI. XIII, fig. 1. 
 
 238 
 
U S. GEOLOGICAL SURVEY. 
 
 BULLETIN No. 62 PLATE XVI 
 
 FIG. I 1X30) 
 
 FI G. 2 ( X30) 
 
 G H.W DEL 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLIHOtS 
 
INDEX 
 
 Page. 
 
 Acid rocks, eruptive, origin of 123 
 
 Actinolite 108, 181 
 
 Adinole 152 
 
 Agglom erates 187 
 
 Albite . . 69,209 
 
 Albite mosaic 60, 156, 210 
 
 . Allanite (see orthite) 118 
 
 Amphibole granite 181 
 
 Amygdaloidal structure 174 
 
 Analyses ... .76, 89, 91, 104, 113, 119, 120, 121, 152, 153 
 
 Anatase 63, 121, 131, 177, 212, 217 
 
 Andesine 114 
 
 Apatite 200 
 
 Aphanitic greenstones 163, 171 
 
 Augengneiss 118,207 
 
 Augen structure 75, 118, 207 
 
 Augen in banded greenstone schists 157 
 
 Augite 139, 175, 200 
 
 B- 
 
 Bald win’s Kilns 
 
 Baltzer, A. cited 
 
 Banded greenstone schists 
 
 Bayley, Prof. W. S.. 
 
 Becko, Fr., cited 
 
 Becker, G. F 
 
 Biotite 
 
 after hornblende 
 
 Bonney, T. G 
 
 Brogger, 'W'. C., cited 
 
 Brook Section 
 
 Brooks, Maj. T. B 
 
 172,178 
 
 44, 47 
 
 154,184 
 
 14, 32 
 
 126,173 
 
 57 
 
 107,108, 200, 212,217 
 
 182 
 
 46 
 
 42, 63 
 
 143 
 
 17, 25, 65, 110, 124 
 
 C. 
 
 Calcite in granites 114, 122 
 
 Carbonates - 214 
 
 Carbonatization 36 
 
 Carp River 175 
 
 Catbrein, A., cited 59, 63, 69, 100, 103 
 
 Chelius, C., cited 50 
 
 Chlorite 55,213 
 
 Chlorite, colorless 73, 79, 105 
 
 Chlorite produced by stretching 83, 164, 
 
 171,176,208 
 
 Chlorite-epidoto aggregate 56, 90, 97, 214 
 
 Cliloritization 55 
 
 Clay slate 124 
 
 Cleveland ore dock, Marquette '58 
 
 Compression 202 
 
 Page. 
 
 j Cores, massive in schist 93 
 
 Credner, H., cited 25, 64, 102, 119 
 
 Cross, W., cited 167 
 
 Cross-gashes (Klaffende Risse) 80. 92, 204 
 
 Crushing 214 
 
 D. 
 
 Dana, J. D., cited 61 
 
 Datbe, cited 57 
 
 DaubrCe, cited 44 
 
 Dead River, Falls of 180 
 
 Deer Lake, agglomerates of 185 
 
 Diabase 138, 183, 197 
 
 glassy 140, 143, 198 
 
 micropegmatitic.. 141 
 
 olivine 138, 143, 180 
 
 tuffs of 133,158 
 
 Diabase Porphyry 198 
 
 Diallage 70, 87, 200, 206 
 
 Diller, J. S , cited 131, 153 
 
 Diorite 146,181,197 
 
 Diorite Porphyry 199 
 
 j Dutton, C. E., cited , 159 
 
 E. 
 
 | Epidiorite 131, 144, 145 
 
 j Epidote (after feldspar) 108, 211 
 
 Epidotization 56 
 
 j Euroka Series, Marquette 137 
 
 F. 
 
 Feldspar 214 
 
 | brown. 103,105,108 
 
 J clear periphery of 79, 90, 103, 108 
 
 deformation of 48, 205 
 
 freshest where crushed 72, 82, 88, 93, 103, 
 
 105, 169, 215 
 
 zonal 117, 148, 178 
 
 | Felsite 122 
 
 I Flaser structure 75, 87, 119, 203 
 
 ; Foliation from join ting 128 
 
 from shearing 129, 142 
 
 Foster and 'Whitney, cited 15, 25 
 
 Four-Foot Falls 123 
 
 G. 
 
 Gabbro 197 
 
 olivine 180, 197 
 
 saussunte 67, 170 
 
 33<J 
 
240 
 
 INDEX, 
 
 Page. ] 
 
 Gabbro-diorite 86 
 
 “ Gabbro Ridge ” of Brooks 77 I 
 
 Garnet 108,210 
 
 Geikie, A., cited 153, 161, 190 
 
 Gneiss 122 
 
 Granite 111,147,178,199 
 
 Granite gneiss : 113, 115, 116 j 
 
 Granite porphyry 117,199 
 
 Granulation, peripheral .. .48, 112, 117, 147, 148, 207 
 
 Great Dyke, Marquette 138 
 
 Groddeck, A. von., cited 62 | 
 
 H. 
 
 Hagge, cited 58 
 
 Harrington B , cited 53 
 
 Heim, A., cited 43, 47 
 
 Helminth 55, 71 
 
 Hitchcock, E., cited 162 
 
 Hornblende 206 
 
 brown 77, 79, 200 
 
 like diallage 102 
 
 surround. ng diallage 70 
 
 sheaf-like 155 
 
 secondary to compact brown 
 
 hornblende after pyroxene 72 78 87, 211 
 
 fibrous, not a secondary enlarge- 
 ment 105, 126, 173, 210 
 
 with granulated center 145 
 
 changing to chlorite 79 
 
 changing to serpentine 109,170 
 
 Horse Race Rapid 96. 106 
 
 I. 
 
 
 
 Ilmenite 200 
 
 altered to sphene 109,217 
 
 stretching of 95, 206 
 
 probable change of, to rutile and mag- 
 netite 99-101 
 
 InostranzefF, cited 54 
 
 Irving, R. D 185 
 
 views of, regarding the Marquette re- 
 gion 19-24 
 
 views of, regarding the Menominee 
 region 29-30, 67 
 
 J. 
 
 M. 
 
 Magnetite 
 
 Marquette. 
 
 Melaphyre 
 
 Metamorphism, defined 
 macro-structural. . . 
 
 micro-structural 
 
 mineralogieal 
 
 Mica 
 
 Microcline 
 
 Microflaser structure . . 
 
 Micropegmatite 
 
 Mortar structure 
 
 Muscovite 
 
 Page. 
 
 200 
 
 134 
 
 198 
 
 36 
 
 43,202 
 
 46,205 
 
 50, 208 
 
 206 
 
 .111,199, 210, 216 
 ..75, 117,170, 176 
 
 141,182 
 
 48, 207 
 
 117,199,212 
 
 N. 
 
 Naumann, C. F., cited 167 
 
 Eegaunee area 171 
 
 Novaculite 151,179 
 
 O. 
 
 Oligoclase 
 
 Olivine 
 
 Olivine diabase . . 
 
 Olivine gabro 
 
 Ophitic structure 
 Orthite 
 
 111,199 
 
 180, 200, 217 
 
 138, 143, 180 
 
 197 
 
 196 
 
 117, 118, 178, 200 
 
 Orthoclase 199 
 
 Orthopinacoid parting in hornblende 103 
 
 Parting, orthopinacoidal 70, 103 
 
 rhomboidal 128 
 
 spheroidal 137, 166, 20,3 
 
 Penfield, S. L., cited 100 
 
 Phillip s, J. A. , cited 161 
 
 Picnic Islands, Marquette 146, 198 
 
 Poicilitic structure 78, 79, 183, 196 
 
 Porphyroids 119 
 
 Pseudo-porphyritic structure 207 
 
 • Pnmpelly, R., cited 67 
 
 Pyroxene 206 
 
 alterations of 216 
 
 change of to hornblende not simple 
 
 paramorphism 52 
 
 Jointing 
 
 Judd, J. W., cited . 
 Julien, A. A., cited 
 
 K. 
 
 Kimhall, J. P., cited 
 Kloos, J. H., cited ... 
 
 L. 
 
 128 
 39, 50 
 146 
 
 i6 
 
 53 
 
 Q. 
 
 Quartz 
 
 broken 
 
 deformation of 
 
 Quartz porphyry 
 
 Quartzite 
 
 Quinnesec, Lower Falls 
 Upper Falls 
 
 199,210 
 
 112 
 
 48, 117, 148, 150, 205 
 
 148,199 
 
 179 
 
 77 
 
 96 
 
 Labradorite 104, 199 
 
 Laspeyres, cited 61 
 
 Lawson, A. C., cited 12, 136, 162, 166, 178 
 
 Lehmann, J., cited 45, 47, 48, 59, 62, 118, 150 
 
 Leucoxene 63, 83 
 
 Lossen, K. A., cited 38, 41, 42, 49, 59, 152, 161 
 
 Lower Quinnesec Falls 77 
 
 R. 
 
 Reusch, H. H., cited 44, 46, 161 
 
 Rhomboidal parting in greenstones 83 
 
 Rominger 18, 19, 27, 06 
 
 Rosenbuscli 49, 52. 55 
 
 Ro hpletz, A., cited 44, 168 
 

 INDEX. 
 
 241 
 
 Rutile 
 
 (thonschiefernadeln) 
 
 after biotite 
 
 after ilmenite 
 
 Page. 
 
 84,91,212 
 
 98,106,212 
 
 115,124,178 
 
 99-101 
 
 Tuffs of diabase 
 
 | acid rocks 
 
 Carp River 
 
 Deer Lake 
 
 Twin Falls 
 
 Page. 
 
 133, 184, 199 
 
 151 
 
 177 8 
 
 185 
 
 127 
 
 s. 
 
 Saussurite 
 
 Saussurite gabbro 
 
 Saussuritization 
 
 Schalstein 
 
 Schenck, A., cited 
 
 Schistose porphyry 
 
 Schmidt, C., cited 
 
 Seri cite 
 
 Sericite schists 
 
 Sericitization 
 
 Serpentine after hornblende 
 
 Shearing 
 
 Sphene .' 
 
 after ilmenite 
 
 Spheroidal parting 
 
 Stelzner, cited 
 
 Stretching, effects of 
 
 Sturgeon Falls 
 
 59,103,210 | 
 67 ! 
 
 54,56 
 
 119 
 
 46, 62 
 
 61,121,212 
 
 74, 84, 88, 105 
 
 60 
 
 .109,170, 214 
 
 129,130,203 
 
 111,200,212,217 
 
 109,182 
 
 137, 166, 203 
 
 121 
 
 ...82, 94,177,188, 204 
 67 
 
 T. 
 
 Talc 107, 214 
 
 Teal Lake 175 
 
 Teall, J. J. H. , cited 46, 53 
 
 Thonschiefernadeln (see rutile) 98, 106, 212 
 
 Titanic iron (see ilmenite) 200 
 
 Tornebohm, A. E., cited 48 
 
 Tourmaline Ill, 112, 114, 124, 200, 206 
 
 U. 
 
 Upper Quinnesec Falls 96 
 
 Upper Twin Falls 132 
 
 Uralite 52 
 
 double zone of, around pyroxene 142 
 
 Uralite diabase 174,175 
 
 Uralitization 52 
 
 V. 
 
 Yan Hise, C. R., cited 
 
 Variolite (?) 
 
 Viridite .. .. 
 
 Vogelsand, H., cited. . 
 
 W. 
 
 ,70,105, 126, 173 
 
 173 
 
 56, 97 
 
 34 
 
 Wadsworth, M. E., cited 17, 5p, 51, 146, 150, 154 
 
 Weathering defined 36 
 
 Weiss, C. E., cited 46,49,150,195 
 
 Whotstone, see novaculite. 
 
 Whetstone brook, Marquette 164 
 
 Wichmann, cited 57, 65, 90, 123 
 
 Wright, C.E 26,123 
 
 Z. 
 
 Zircon ... Ill, 113, 122, 124, 200, 206 
 
 Zoisite 69, 102, 184, 210 
 
Title for subject entry. Author title. Series title. 
 
 LIBRARY CATALOGUE SLIPS. 
 
 United States. Department of the interior. ( XJ. S. geological survey). 
 
 Department of the interior J — | Bulletin | of the | United 
 States j geological survey | no. 63 | [Seal of the department] | 
 
 Washington | government printing office | 1890 
 
 Second title: United States geological survey | J. W. Powell, 
 director | — | A bibliography | of | paleozoic Crustacea | from | 
 1698 to 1889 | including a list of north american species and a | 
 systematic arrangement of genera | by | Anthony W. Vogdes ] 
 [Vignette] | 
 
 Washington | government printing office j 1890 
 
 8°. 177 pp. 
 
 Vogdes (Anthony Wayne). 
 
 United States geological survey | J. W. Powell, director | — | 
 A bibliography | of | paleozoic Crustacea | from | .1698 to 1889 | 
 including a list of north american species and a | systematic ar- 
 rangement of genera | by | Anthony W. Vogdes | [Vignette] | 
 Washington | government printing office | 1890 
 8°. 177 pp. 
 
 [United States. Department of the interior. ( TJ . S. geological survey). 
 
 Bulletin 63] . 
 
 United States geological survey | J. W. Powell, director | — | 
 A bibliography | of | paleozoic Crustacea | from | 1698 to 1889 | 
 including a list of north american species and a | systematic ar- 
 rangement of genera | by | Anthony W. Vogdes | [Vignette] | 
 Washington | government printing office | 1890 
 6°. 177 pp. 
 
 [United States. Department of the interior. (TJ. S. geological survey). 
 
 Bulletin 63]. 
 
ADVERTISEMENT. 
 
 [Bulletin No. 63.1 
 
 The publications of the United States Geological Survey are issued in accordance with the statute 
 approved March 3, 1879, which declares that — 
 
 • ‘ The publications ofthe Geological Survey shall consist of the annual report of operations, geological 
 and economic maps illustrating the resources and classification of the lands, and reports upon general 
 and economic geology and paleontology. The annual report of operations of the Geological Survey 
 shall accompany the annual report of the Secretary of the Interior. All special memoirs and reports 
 of said Survey shall he issued in uniform quarto series if deemed necessary by the Director, but other- 
 wise in ordinary octavos. Three thousand copies of each shall be published for scientific exchanges 
 and for sale at the price of publication ; and all literary and cartographic materials received in exchange 
 shall be the property of the United States and form a part of the library of the organization : And the 
 money resulting from the sale of such publications shall be covered into the Treasury of the United 
 States.” 
 
 On July 7, 1882, the following joint resolution, referring to all Government publications, was passed 
 by Congress: 
 
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IV 
 
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DEPARTMENT OF THE INTERIOR 
 
 BULLETIN 
 
 OF THE 
 
 UNITED STATES 
 
 * 
 
 GEOLOGICAL SURVEY 
 
 NTo. 63 
 
 WASHINGTON 
 GOVERNMENT PRINTING OFFICE 
 1890 
 
UNITED STATES GEOLOGICAL SURVEY 
 
 J. W. POWELL, DIRECTOR 
 
 A BIBLIOGRAPHY 
 
 OF 
 
 PALEOZOIC CKITSTACEA 
 
 FROM 
 
 1698 to 1889 
 
 INCLUDING A LIST OF NORTH AMERICAN SPECIES AND A 
 SYSTEMATIC ARRANGEMENT OF GENERA 
 
 BY 
 
 ANTHONY W. VOGDES 
 
 WASHINGTON 
 
 GOVERNMENT PRINTING OFFICE 
 1890 
 
‘ CONTENTS. 
 
 Letter of transmittal 
 
 Introduction 
 
 I. List of authors 11 
 
 II. Catalogue of trilobites 79 
 
 III. Catalogue of non-trilobites 149 
 
 5 
 
 
Department of the Interior, 
 
 United States Geological Survey, 
 Division of Paleozoic Invertebrate Paleontology, 
 
 Washington, D. G., May 1, 1890. 
 
 LETTER OF TRANSMITTAL. 
 
 Sir: I have the honor to transmit herewith, for publication, a bibli- 
 ography of Paleozoic Crustacea, prepared by Lieutenant A. W. Vogdes, 
 
 The bibliography bears internal evidence of long continued and ex- 
 tended research and its publication will supply a work of reference 
 that has long been needed by the student of invertebrate Paleozoic 
 fossils. 
 
 I remain, very respectfully, 
 
 U. S. A. 
 
 Chas. D. Walcott, 
 
 Paleontologist. 
 
 Hon. J. W. Powell, 
 
 Director U . 8. Geological Survey. 
 
INTRODUCTION. 
 
 The sole object of this bulletin is to give a general view of the litera- 
 ture on the Paleozoic Crustacea and to aid students and paleontologists 
 in their researches. It is the result of more or less constant work 
 during the past ten years. 
 
 In its compilation I have examined almost every reference before re- 
 cording it; those not so examined are indicated by a star (*) follow- 
 ing the title. 
 
 For convenience, the subject-matter has been arranged as follows: 
 
 Part I. List of authors, including a brief index of the genera de- 
 scribed in each work. 
 
 Part II. A catalogue of the North American Paleozoic trilobites. 
 
 Part III. The non-trilobitic Paleozoic Crustacea, with a list of the 
 species. 
 
 I am well aware that the value of a work of this kind depends upon 
 the care and labor given to its compilation. Every possible means of 
 obtaining accurate information from a miscellaneous class of literature 
 in many languages has been used, and it is hoped that there are but 
 few errors and omissions. 
 
 I would thank those into whose hands this bulletin may fall for any 
 information that would add to its value as a working hand-book, 
 
 A. W. Vogdes. 
 
 Fort Hamilton, New York Harbor, April 30, 1889. 
 
 9 
 
PART I. 
 
 LIST OF AUTHORS. 
 
A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA FROM 1698 TO 1889, 
 
 INCLUDING 
 
 A LIST OP NORTH AMERICAN SPECIES AND A SYSTEMATIC ARRANGEMENT OP GENERA. 
 
 By Anthony W. Vogdes. 
 
 PART I. 
 
 LIST OF AUTHORS. 
 
 A star (*) following a title indicates that the reference is recorded without opportunity for personal 
 
 verification. 
 
 Agassiz (L.) Monographic des poissons 
 fossiles du vieux gres rouge oil systeme 
 d6vonien (old Red Sandstone) des lies 
 Britanniques et de Russie. 
 
 Text, Soleure; atlas, Neuch&tel, 1845, pp. 
 xix-xx, notd; and atlas, Tab. A. 
 
 Pterygotus n. g. 
 
 Alth (Alois von). Ueber die palaeozoi- 
 schen Gebilde Podoliens und deren Ver- 
 steinerungen. Erste Abtheilung. 
 
 In Abhandl. k. k. geol. Reichsanst., vol. 7, 
 pt. 1, Wien, 1874, 5 pi. 
 
 Proetus , Gyphaspis, Dalmania , Calymene, 
 Ceraurus , Sphcerexochus, Encrinurus , lllcenus, 
 Eurypterus, Pterygotus, Stylonurus, Beyrichia, 
 Leperditia, Primitia, Bairdia. 
 
 Alton (Ed. de). See Burmeister and 
 Alton. 
 
 Ami (Henry M. ) Notes on Triarthrus 
 8pino8M Billings. 
 
 In Trans. Ottawa Field Nat. Club, No. 4, 
 18i*2-'83, p. 88, 1 pi. 
 
 Angelin (N. P.) Palseontologia Scandi- 
 navica. Pars I. Crustacea formationis 
 transitionis. Lipsite, 1854, 4to. 
 
 The first part of this work, entitled “Palae- 
 ontologia Scandinavica,” containing pp. 1-24 and 
 pi. 1-24, was published by the Royal Swedish 
 Academy of Sciences in 1852. The second por- 
 tion in 1854, including a preface, pp. 1-9 and pp. 
 21-92, pi. 25-42. 
 
 The genera are arranged in the following 
 order: Olenus, Paradoxides, Gryptonynus, Eryx | 
 
 Angelin (N. P.) — Continued. 
 
 n. g. (corrected by Angelin to Elyx, the ge- 
 neric term Eryx having been used by Stephen 
 in 1832 for a genus of the Coleoptera), Acontheus 
 n. g. (corrected by the author to that of Aneu- 
 canthus), Agnostus, Phacops, Polytomurus , Re- 
 mopleurides, Niobe n. g., Megalaspis n. g., Nileus, 
 Ampyx, Proetus, Plicethonides (Angelin uses this 
 term for that of Phaeton Barr.), Forbes-ia, Gonio- 
 pleura, Celmus n. g., Anomocare n. g., Soleno- 
 pleura n. g., Liostracus n. g., Calymene, Homa- 
 lonotus, Pliomera ( Amphion ), Cheirurus, Cyrto- 
 metopus n. g., Acidaspis, Trapelocera, Sphce- 
 rexochus, Acidaspis, Rhodope n. g. (this term 
 was used by Siebold in 1848 for a genus of the 
 Gasteropoda), Dysplanus, Bumastus, lllcenus, 
 JEglina, Olenus , Peltura, Parabolina, Acerocare 
 n. g., Leptoplastus n. g., Eurycare n. g. (this 
 genus is referred by J. W. Salter, Mem. Geol. 
 Survey United Kingdom, Brit. Organic Re- 
 mains, decade xi, pi. 8, p. 3, to the genus Splice - 
 rophthalmus Ang.), Sphcerophthalmus n. g., 
 Anopocare n. g. (this genus is referred by J. G. O. 
 Linnarsson, Geol. Fbrening. Stockholm Forhdl., 
 vol. 5, 1880— ’81, p. 136, to the genera Peltura and 
 Sphcerophthalmus; the specimen, according to 
 Dr. Linnarsson, in the Royal Museum of Swollen, 
 “marked by Angelin as the abdomen till Stenom. 
 pusillus, contains several small heads of Sphce- 
 rophthalmus alatus, and a small pygidium of 
 Peltura scarabceoides Dr. Linnarsson refers to 
 this specimen as Angelin’s typo for the genus 
 Anopocare and also remarks “that Angelin in- 
 tended to change the family name of Sphceroph- 
 thalmu8 alatus and their nearest forms to that 
 of Stenometopus, inasmuch as another speci- 
 men of Sph. alatus has, in Angelin’s own hand- 
 
 13 
 
14 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63 . 
 
 Angelin (N. P.) — Continued. 
 
 writing, the generic name of Stenometopus"), 
 Ptychopyge n. g., Asaphus, Bronteus, Holome- 
 topu8 n. g., Isocolus, Corynexochus n. g., Sym- 
 physurus, Euloma n. g., Pharostoma , Cono- 
 coryphe. Trinucleus, Sphcerexocoryphe n. g., Dei- 
 phon, Staurocephalus , Lichas, Dolichometopus 
 n. g., Platymetopus, Cyrtometopus, Ampyx, 
 Jlaphiophorus, Lonchodomas, Harpes , Arraphus 
 n. g., Harpides, Centropleura n. g. (J. G. O. Lin- 
 narsson, Svenska Yetensk. Akad. Handl., vol. 8, 
 1869, No. 2, p. 71, cites Angelin’s Centropleura 
 angusticauda and C. dicrceura under Dr. Owen’s 
 genus Dikelocephalus ) , Cybele, Telephus, Ogygia , 
 Ogygiocaris n. g. 
 
 Palseontologia Scandinavica. Pars I. 
 
 Crustacea formationis transitionis fas- 
 ciculi 1 et 2 cum tabulis 48. Holmiae, 
 1878 (3d ed.). 
 
 This work contains plates 1, la, 2, 3, 20, 22, 
 with an appendix, pp. 93-96. Emended and re- 
 vised by Prof. Gustaf Lindstrdm. 
 
 The appendix contains descriptions and fig- 
 ures of the following species: Paradoxides tes- 
 sini, P. tessini var. wahlenbergii, P. tessini var. 
 celandicus, P. affinis, P. tuber culatus, P. forch- 
 hammeri, P. tumidus, Centropleura loveni, C. 
 steenstmpi, Ogygiocaris dilatata, O. dilatata 
 var. sarsi, 0. dilatata var. str'omi, in addition 
 to the genera and species described in the 
 second edition. 
 
 Anthony (J. G.) New Trilobites. 
 
 In Am. Jour. Sci., 1st series, vol. 34, 1838, p. 
 379. 
 
 Ceratocephala ceralepta, figs. 1 and 2. 
 
 Description of a new fossil {Calymene 
 
 bucklandii). 
 
 In Am. Jour. Sci., 1st series, vol. 36, 1839, p. 
 106. 
 
 In this article a specimen of Ceraurus pleur- 
 exanthemus Green was figured and described 
 under the name of Calymene bucklandii as a 
 new species. 
 
 Audouin ( J. Y. ) Recherches sur les 
 rapports uaturels qui existent entre les 
 Trilobites et les animaux articul^s. 
 
 In Annales G6n. Sc. Phys. Nat., Bruxelles, 
 vol. 8, 1821, pi. 18, p. 233 ; also Isis (Oder Encyc. 
 Zeitung), Oken, vol. 1, 1822, p. 87. 
 
 Calymene blumenbachii. 
 
 Baily (W. H.) On two new species of 
 Crustacea ( Belinurus Kiinig) from the 
 Coal Measures in Queen’s County, Ire- 
 land ; and some remarks on forms allied 
 to them. 
 
 In Rept. 28th Meeting Brit. Assoc. Adv. Sci., 
 1858, p. 76. 
 
 On the annuloid Crustacea of the 
 
 Coal Measures. (*) 
 
 In Jour. Geol. Soc. Dublin, vol. 8, 1858, p. 89. 
 
 In this paper a description of a fossil Crusta- I 
 
 Baily (W. H.) — Continued. 
 
 cean from the Rilboa Colliery, Queen’s County, 
 was given, with a few remarks on the allied 
 species from Coal Brook Dale, which had been 
 included with it in the genus Limulus, and it 
 was proposed to remove all these Coal-Measure 
 Crustacea from that genus and group them 
 into a new one, under the name of Steropis. 
 
 Remarks on some Coal-Measure Crus- 
 tacea belonging to the genus Belinurus 
 Kdnig, with descriptions of two new 
 species from Queen’s County, Ireland. 
 PI. 5. 
 
 In Annals Nat. Hist., 3d series, vol. 2, 1863, p. 
 105. Translated by Milne- Edwards, Annales 
 G6n. Sc. Phys. Nat., Bruxelles, 1863. 
 
 The author herein describes Belinurus re • 
 gin.ce , B. arcuatus , B. bellulus, B. rotundus ? 
 
 Charles Konig in his work (leones Fos- 
 silium Sectiles, London, 1825) simply mentions 
 the name of Belinurus bellulus in his explana- 
 tion of pi. 18, fig. 230. 
 
 Figures of characteristic British fos- 
 sils, with descriptive remarks. 
 
 Pt. 1, pis. 1-10, Cambrian and Lower Silu- 
 rian, London, 1867; pt. 2, pis. 11-20, 1869; pt. 
 3, pis. 21-30, 1871. 
 
 Paradoxides, Dikelocephalus? , Olenus, Palceo- 
 pyge, Conocoryphe , Angelina , Proetus , Phacops, 
 Calymene, Homalonotus, Lichas , Trinucleus, 
 Ampyx , Asaphus, Ogygia, Niobe, Psilocephalus, 
 ASglina, Cheirurus , Sphcerexochus, Encrinurus, 
 Illoenus , Agnostus, Eurypterus , Pterygolus, 
 Ceratiocaris, Beyrichia, Cythere, Primitia, 
 Hymenocaris. 
 
 On Trilobites and other fossils from 
 
 Lower or Cambro-Silurian strata in the 
 county of Clare. (*) 
 
 In Jour. Royal Geol. Soc. Ireland, vol. 17, pt. 
 1, 1886, p. 29. 
 
 Banks (R. W.) On the tilestones or- 
 Downton sandstones, in the neighbor- 
 hood of Kington, and their contents. 
 
 In Quart. Jour. Geol. Soc. London, vol. 12, 
 1856, p. 93, plate. 
 
 Pterygotus, Pteraspis, Eurypterus, Hunan- 
 top ter us. 
 
 Barrande (Joachim). Notice pr61imi- 
 naire sur le systkme silurien et les Tri- 
 lobites de Boberne. Leipsic, 1846. 
 
 Etage C : Paradoxides, Conocephalus, Ellipso- 
 cephalus , Arion n. g., Sao n. g., Baltus, Hydro- 
 cephalus n. g., Monadina n. g. 
 
 Etage D : Phacops, Calymene, Odontopleura, 
 Asaphus, Cheirurus, Trinucleus , Caphyra n g., 
 Dione n. g., Illcenus, Egle n. g., Battus. 
 
 Etage E : Phacops, Arethusa n. g., Sphcerexo- 
 chus, Asaphus, Cheirurus, Calymene, Stauro- 
 cephalus n.g., Lichas, Harpes, Odontopleura , 
 Cyphaspi8, Bronteus , Phceton n. g., Proetus. 
 
VODGES.] 
 
 LIST OF AUTHORS. 
 
 15 
 
 Barrande (Joachim) — Continued. 
 
 32tage F : Phacops, Bronteus, Lidias, Proetus, 
 Harpes, Cheirurus, Odontopleura, Cyphaspis. 
 
 35 tage G : Phacops , Bronteus, Cheirurus, Cy- 
 phaspis, Odontopleura, Proetus. % 
 
 Nouveaux Trilobites. Supplement h 
 
 la Notice prdliminaire sur le syst&me 
 silurien et lea Trilobites de Boheme. 
 Prague, 1846. 
 
 Etage C : Schistes fossiliferes. 
 
 Etage D : Cheirurus, Phacops, Ampyx, Gdon- 
 topleura, lllcenus. 
 
 Etage E: Arethusa, Harpes. 
 
 Etage F : Proetus, Phceton, Bronteus, Odon- 
 topleura. 
 
 Etage G : Harpes, Cheirurus, Phacops. 
 
 UeberdasHypostomaundEpistoma, 
 
 zwei analoge aber verschiedene Organe 
 der Trilobiten. 
 
 In Neues Jahrbucli fur Mineral., 1847, p. 885, 
 pi. 8. 
 
 Phacops sodalis, P. breviceps, Amphion, II- 
 Icenus, Cheirurus, Asaphus, Lichas. 
 
 The generic term Dione is herein modified to 
 that of Dionide, p. 391. 
 
 Sao hirsuta Barrande, ein Bruch- 
 
 stuck aus dem “Syst&me silurien du 
 centre de la Boheme.” 
 
 In Neues Jahrhuch fiir Mineral., 1849, p. 385, 
 pi. 7. 
 
 Sao. 
 
 Note on Trilobites. 
 
 In Ber. Mittheil. Freunde Naturw., "Wien, 
 vol. 4, 1849, p. 353. 
 
 Noticed by J. "W. Salter. 
 
 In Quart. Jour. Geol. Soc. London, vol, 6, 1849, 
 pt. 2, p. 34. 
 
 Deiphon forbesii , neuer Trilobit aus 
 
 Bohmen. 
 
 In Ber. Mittheil. Freunde Naturw., "Wien, 
 vol. 5, 1850, p. 6. 
 
 Versuch einer Klassification der Tri- 
 lobiten. 
 
 In Neues Jahrhuch fiir Mineral., 1850, p. 769. 
 
 Syst&me silurien du centre de la 
 
 Boheme. l re partie. Recherches pald- 
 ontologiques. Prague et Paris, 1852. 
 
 Yol. 1. Text, Crustac6s, Trilobites. With 
 atlas of 51 pis. 
 
 This classical work contains a historical 
 sketch of all the genera of Trilobites, and de- 
 scriptions of the following genera: 
 
 Harpes, Remoplcurides, Paradoxides, Hydro- 
 cephalus, Sao, Arionellus n. g., Ellipsocephalus, 
 Olenus, Peltura, Triarthrus, Conocephalites, 
 Proetus, Phillipsia, Griffithides, Cyphaspis, Are- 
 thusina (generic term changed from that of 
 Arethus to Arethusina), Harpides, Phacops, 
 Dalmanites, Calymene, Homalonotus, Lichas, 
 Trinucleus, Ampyx, Dionide (generic term 
 
 Barrande (Joachim)— Continued. 
 
 changed from Dione to Dionide), Asaphus, 
 Ogygia, Mglina n. g., lllcenus, Nileus, Sym- 
 physurus, Acidaspis, Cheirurus, Placoparia, 
 Sphcerexochus, Staurocephalus, Deiphon, Dindy- 
 mene, Zethus, Amphion . Encrinurus, Cromus 
 n. g., Bronteus, Agnostus, Telephus n. g. 
 
 On Ceratiocaris bohemicus. 
 
 In Neues Jahrhuch fiir Mineral., 1853, pt. 3, 
 pp. 335-347. 
 
 On p. 335 of this article there is a review of 
 Dr. D. D. Owen’s Kept. Geol. Survey Wiscon- 
 sin, Iowa, and Minnesota, Phila., 1852. 
 
 ? Dicalocephalus , etc. 
 
 — — Note sur quelques nouveaux fossiles 
 ddcouverts aux environs de la ville de 
 Rokitzan dans le bassin silurien du 
 centre de la Boheme. 
 
 In Bull. Soc. G6ol. France, 2d series, vol. 13, 
 1856, p. 532. 
 
 Calymene. Placoparia, Acidaspis, Agnostus, 
 Amphyx, Harpes, Ogygia. 
 
 Mere mention of locality and period. 
 
 Wiedererscheinung der Gattung^Ire- 
 
 thusina Barrande. 
 
 In Neues Jahrhuch fiir Mineral., 1858, p. 257, 
 
 1 pi. 
 
 Arethusina sandbergeri Barr. 
 
 Documents anciens et nouveaux sur 
 
 la faune primordiale et le SystSme 
 Taconique en Amdrique. 
 
 In Bull. Soc. G6ol. France, 2d series, vol. 18, 
 1861, pp. 203-321, pis. 4, 5. 
 
 Paradoxides asaphoides Emmons, P. thomp- 
 soni Hall, P. macrocephalus Emmons, P. ver- 
 montana Hall, Peltura ( Olenus ) holopyga Hall, 
 Atops trilineatus Emmons, A. punctatus Em- 
 mons, Triarthrus bedci Green, Microdiscus 
 quadrico status Emmons. 
 
 I. Rdapparition du genera Arethu- 
 sina Barrande. II. Faune silurienne 
 des environs de Hof, en Bavidre. 
 Prague et Paris, 1868. 
 
 Olenus, Conocephalites, Arethusina, Caly- 
 mene, Bavarilla n. g., Lichas , Asaphus, Cheiru- 
 rus, Agnostus. 
 
 Trilobites. I. Rdsumd gdndral de 
 
 nos dtudes sur Involution des Trilo- 
 bites. II. Distribution verticale des 
 Trilobites dans le bassin silurien de la 
 Boheme. III. Paralldle entre les Tri- 
 lobites et Cdphalopodes siluriens de la 
 Boheme. IV. Flpreuve des tlidories pa- 
 ldontologiquos par la rdalitd. Prague 
 et Paris, 1871. 
 
 Systdme silurien du centre de la 
 
 Bobdme. l re partie. Recherches pa- 
 ldontologiques. Supplement au vol. 1. 
 
16 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 ' iBULL. 63. 
 
 Barrande (Joachim)— Continued. 
 Trilobites. Crustac^s di vers et poissons. 
 Prague et Paris, 1^72, 32 pis. 
 
 Trilobites. Harpes, Remopleurides , Paradoxi- 
 des, Plutonia, Anopolenus, Dikelocephalus, Doli- 
 chometopus, Hydrocephalus , Olenus, Olenellus, 
 Bohemilla , Conocephalites, Aneuacanthus, An- 
 gelina, Anomocare, Arionellus, Atops, Bathyu- 
 rus, Ghariocephalus, Corynexochus, Ellipsoce- 
 phalus, Holocephalina, Ptychaspis, Sao, Triar- 
 thrus, Triarthrella, Proetus, Arethurina, Gar- 
 mon n. g., Cyphaspis, Cyphoniscus, Harpides, 
 Isocolus , Phillipsia . Phacops, Dalmanites, Caly- 
 mene, Pavarilla, Homalonotus, Lichas, Trinu- 
 cleus, (Lmpyx, Dionide, Endymionia, Microdis- 
 cus, Asaphus, Barrandia, Ogygia, Psiloceplialus, 
 Stygina, JEglina, Illcenurus, Acidaspis, Cheiru- 
 rus, Areia, Crotalurus, Deiphon, Placoparia, 
 Sphcerexochus, Staurocephalus, Zethus, Dindy- 
 mene, Amphion,Cromus, Encrinurus, Bronteus, 
 lllcenus, Nileus, Agnostus, lllcenopsis, Pemphi- 
 gaspis, Shumardia , Telephus n. g., Tnopus. 
 
 Phyllopoda. Geratiocaris, Aptychopsis n. g., 
 Cryptocaris n g M Pterocaris n. g. 
 
 Ostracodes. Aristozoe u. g., Beyrichia, Bol- 
 bozoe n. g., Callizoe n. g., Caryon n. g., Grescen- 
 tilla a. g., Cythere , Cytheropsis n. g., Elpc n. g , 
 Entomis, Hippa n. g., Isochilina, Leperditia, 
 Nothszoe u. g., Orozoe n. g., Primitia, Zonozoe 
 n. g. 
 
 Eurypteridae. Pterygotus, Eurypterus. 
 
 Cirrhipedise. Anatifopsis n. g., Plumulites n. 
 g., Bactropus n. g , Dryalus n. g. 
 
 See Oorda (A. J. C.) and Hawle (Ignaz),* 
 
 and Verneuil (E. de). See Verneuil 
 
 (E. de) and Barrande (Joachim). 
 
 Barrett (S. T.) The coralline or Niagara 
 limestone of the Appalachian system as 
 represented at Nearpass’s Cliff, Mon- 
 tague, N. J. 
 
 In A®. Jour. Sci., 3d series, vol. 15, 1878, p. 
 370. 
 
 Proetus pachydermatus n. s. 
 
 Description of a new Trilobite, Dal- 
 manites dentata. 
 
 In Am. Jour. Sci., 3d series, vol. 11, 1876, p. 
 200, plate. 
 
 On Dalmanites dentata. 
 
 In Am. Jour. Sci., 3d series, vol. 12, 1876, p. 70. 
 
 Barris (W. H.) New fossils from the 
 Corniferous formation at Davenport. 
 
 In Davenport Acad. Nat. Sci., vol. 2, 1879, p. 
 282, pis. 10 and 11. 
 
 Proetus davenportensis n. s., pi. 11, fig. 8. 
 
 Barrois (Charles). Note sur des fossiles 
 de Catheryielle. 
 
 In Bull. Soc. G6ol. France, 3d series, vol. 8, 
 
 1880, p. 266. 
 
 Phacops fecundus, Dalmanites hausmani, 
 
 pi. 8. 
 
 Barrois (Charles) — Continued. 
 
 Recherches sur les terrains anciens 
 
 des Asturies et de la Galice. 
 
 In M6m. Soc. G6ol. Nord, Lille, vol. 2, 1882, 
 (*30 pp., 20 pis. 
 
 Paradoxides, Conocephalus, Arionellus. 
 
 Sur les faunes siluriennes de la 
 
 Haute-Garonne. Pis. 6, 7. 
 
 In Annales Soc. G6ol. Nord, Lille, vol. 10, 
 1883, p. 151. 
 
 Cyphaspis, Phacops, Dalmanites, Lichas. 
 
 Les appendices des Trilobites. 
 
 In Annales Soc. G6ol. Nord, Lille, vol. 11, 
 1883- 84, p. 228. 
 
 Memoire sur le calcaire & Polypiers 
 
 de Cabri&res (H6rault). 
 
 In Annales Soc. G6ol. Nord, Lille, vol. 13, 
 1885-’86, p. 74, plate. 
 
 Phacops, Bronteus. 
 
 Sur la faunede Haut-de-Ver (Haute- 
 
 Garonne). 
 
 In Annales Soc. G6ol. Nord, Lille, vol. 13, 
 1885- ’86, pis. 2,3. 
 
 Harpes, Cyphaspis, Phacops, Dalmanites, 
 Lichas , Bronteus. 
 
 Sur le calcaire ddvonien de Chaude- 
 
 fonds (Maine-et-Loire). 
 
 In Annales Soc. G6ol. Nord, Lille, vol. 13, 
 1885-’86, p. 170. 
 
 Aper^u de la constitution g^ologique 
 
 de la rade de Brest. 
 
 In Bull. Soc. G6ol. France, 3d series, vol. 14, 
 1886, p. 678, pis. 31-33. 
 
 Homalonotus le Hiri Barrois. 
 
 Baumer (J. W.) Naturgeschichte des 
 Mineralreichs mit besonderer Anwen- 
 dung auf Thiiringen. 2 vols. Gotha, 
 1763-64, 1767. 
 
 Bayle (E.) Explication de la carte gdo- 
 logique de la France. Yol. 4. Atlas. 
 Paris, 1878. 
 
 Premiere partie. Fossiles principaux des 
 terrains. 
 
 PI. 1, Megalaspis ; pi. 2, Homalonotus,- pi. 3, 
 Galymene pi. 4, Gheirurus , lllcenus, Phacops, 
 Cryphceus, Goldius, Proetus, Phillipsia; pi. 5, 
 Acidaspis. 
 
 Bean (W.) Entomostracans from the 
 Coal Measures of Newcastle-upou-Tyne. 
 
 In Mag. Nat. Hist. (London), vol. 9, 1836, p. 
 376. 
 
 Beyrichia. 
 
 Beckmann (J.) Commentatio de reduc- 
 tione rerum fossilium ad genera natu- 
 ralia protyporum. 
 
 In Novi Comm. Soc. Scient. Gotting., vol. 3, 
 1773, p. 95. 
 
•‘'OGDEB.J 
 
 LIST OF AUTHORS. 
 
 17 
 
 Beecher (C. E.) Ceratiocaridce from the 
 Upper Devonian Measures in Warren 
 County. 
 
 In Second Geol. Survey Pennsylvania, vol. 
 PPP, 1884, 2 pis. 
 
 Echinocaris, Elymocaris n. g., Tropidocaris 
 n. g. 
 
 Author’ s edition issued separately, entitled: 
 “ Ceratiocaridce from theChemung and Waverly 
 Groups at "Warren, Pa.,” with 2 pis., Harris- 
 burg, 1884, 22 pp. 
 
 Belt (Thomas). On some new Trilobites 
 from the Upper Cambrian rocks of North 
 Wales. 
 
 In Geol. Mag., vol. 4, London, 1867, p. 294, pi. 
 
 12 . 
 
 Agnostus pisiformis, A. nodosus, Olenus gib- 
 bosus. 
 
 On the Lingula flags or Festiniog 
 
 group of the Dolgelly district. 
 
 In Geol. Mag., vol 5, London, 1868, p. 5, pi. 2. 
 
 Conocoryphe, Sphcerophthalmus , Agnostus. 
 
 Bergeron (M.-T.) Etude paldontologi- 
 que et stratigraphique des terrains 
 anciens de la montagne Noire. 
 
 In Bull. Soc. G6ol. France, 3d series, vol. 15, 
 1887, No. 5. 
 
 Harpes, Phacops, Cheirurus. 
 
 Beushausen ( Louis ). Beitrage zur 
 Kenntniss des oberharzer Spiriferen- 
 sandsteins und seiner Fauna. (*) 
 
 Inaugural-Dissertation. Gottingen, 1884, p. 
 34. 
 
 Beyrich (Ernst). Ueber einige bohmi- 
 sche Trilobiten. Berlin, 1845, 1 pi. 
 
 Lichas, Cheirurus n. g., Sphcerexochus n. g., 
 Bronteus , Battus, Trochurus n. g. 
 
 Untersuchungen iiber Trilobiten. 
 
 Zweites Stuck als Fortsetzung zu der 
 Abhandlung “Ueber einige bohmische 
 Trilobiten.” Berlin, 1846, 3 pis. 
 
 Harpes. Harpid.es n. g., Proetxis, Calymene, 
 Lichas. Trinucleus. Odontopleura, Cheirurus , 
 Sphcerexochus. Arges, Bronteus. 
 
 Bigsby (J. J.) Description of a new 
 species of Trilobite. 
 
 In Jour. Acad. Nat. Sc. Phila., vol. 4, pt. 2, 
 1825, p. 365, pi. 23. 
 
 Paradoxides boltoni ( Lichas boltoni). 
 
 ■ Thesaurus Siluricus. The flora and 
 
 fauna of the Silurian period. London, 
 
 1868 . 
 
 Billings (E ) Fossil foot prints. 
 
 In Canadian Naturalist, vol. 1, 1856, p. 35, 
 wood-cuts. 
 
 Protichnites septem notatus. 
 
 ■ On some of the characteristic fossils 
 
 of the Lower Silurian rocks of Canada. 
 
 Bull. 63 2 
 
 Billings (E.)— Continued. 
 
 In Canadian Naturalist, vol. 1, 1856, p. 39, 11 
 wood- cuts. 
 
 The author figures Isotelus gigas , Calymene 
 senaria, and the hypostoma of Isotelus gigas. 
 
 — — Fossils of the Upper Silurian rocks, 
 Niagara and Clinton groups. 
 
 In Canadian Naturalist, vol. 1, 1856, p. 57, 1 pi. 
 
 Phacops limulurus Green. 
 
 Description of fossils occurring in 
 
 the Silurian rocks of Canada. 
 
 In Canadian Naturalist, vol. 1, 1856, p. 312, 10 
 wood-cuts. 
 
 Homalonotus delphinocephalus Green. 
 
 Report for the year 1856 of E. Bil- 
 lings, esq., palaeontologist, addressed 
 to Sir Wm. E. Logan, etc. 
 
 In Geol. Survey Canada. Kept, Progress, 1853- 
 ’54-’55-’56, p. 247. 
 
 Triarthrus spinosus n. s., Acidaspis horani 
 n. s., Bronteus lunatus n. s. 
 
 Fossils of the Calciferous saudrock, 
 
 including those of a deposit of white 
 limestone at Mingau, supposed to be- 
 long to the formation. 
 
 In Canadian Naturalist, vol. 4, 1859, p. 345, 12 
 wood cuts. 
 
 Bathyurus n. g., Leperditia. 
 
 Description of some new species of 
 
 Trilobites from the Lower and Middle 
 Silurian rocks of Canada. 
 
 In Canadian Naturalist, vol. 4, 1859, p. 367, 18 
 wood-cuts. 
 
 Triarthrus, Amphion, lllcenus. 
 
 Fossils of the Chazy limestone, with 
 
 descriptions of new species. 
 
 In Canadian Naturalist, vol. 4, 1859, p. 426, 38 
 wood-cuts. 
 
 Harpes, Bathyurus, Leperditia. 
 
 Description of some new species of 
 
 fossils from the Lower and Middle Silu- 
 rian rocks of Canada. 
 
 In Canadian Naturalist, vol. 5, 1860, p. 49, 16 
 wood-cuts. 
 
 Proetus, Phacops, Dalrnanites, Cheirurus. 
 
 On some new species of fossils from 
 
 the limestone near Point Levi, opposite 
 Quebec. 
 
 In Canadian Naturalist, vol. 5, I860, p. 301, 30 
 figs. 
 
 Dikelocephalus , Conocephalites, Arionclhis, 
 Bathyurus , Menocephalus, Asaphus, Cheirurus, 
 Agnostus. 
 
 On some of the rocks and fossils 
 
 occurring near Phillipsburg, Canada 
 East. 
 
 In Canadian Naturalist, vol, 6, 1861, p. 310, 6 
 figs. 
 
 Bathyurus, Menocephalus, Amphion. 
 
18 
 
 [bull. 63. 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Billings (E.) — Continued. 
 
 On some new or little-known species 
 
 of Lower Silurian fossils from the Pots- 
 dam group (Primordial zone). Mon- 
 treal, 1861, 24 pp. 
 
 Tliis pamphlet, with the addition of a de- 
 scription of Archceocyathus profundus, the sup- 
 pression of that of A. minganensis, and the 
 notes on pages 10, 11, and 12, was reprinted in 
 the “Palaeozoic Fossils of Canada,” vol. 1, 
 1865, pp. 1-24, also in part in the “Geol. Ver- 
 mont, ” vol. 2, 1861, pp. 942-960. 
 
 Olenellus thompsoni Hall, Olenellus vermon- 
 tana Hall, Oonocephalites miser n. s., C. adamsi 
 n. -s., 0. teucer, O. vulcanus n. s., C. arenosus n. 
 s., Bathyurus senectus n. s., B. parvulus n. s., 
 Ampyx halli n. s. 
 
 Description of a new species of 
 
 Harpes from the Trenton limestone, 
 Ottawa. 
 
 In Canadian Naturalist, vol. 8, 1863, p. 36, 
 wood-cut. 
 
 Harpes dentoni n. s. 
 
 Geological Survey of Canada. Re- 
 port of progress from its commence- 
 ment to 1863. Illustrated by 498 wood 
 cuts in the text. Montreal, 1863. Atlas 
 of maps and sections. 
 
 Harpes, Paradoxides, Conocephalites, Triar- 
 thrus, Bathyurus, Proetus, Phaeops, Dalma- 
 nites, Calymene, Lichas, Trinucleus , Asaphus, 
 Illamus, Acidaspis , Gheirurus, Amphion , En- 
 crinurus, Bronteus, Beyrichia, Leperditia, 
 Isochilina, Eurypterus, Gytheropsis. 
 
 — Description of new species of Phil- 
 lipsia from the Lower Carboniferous 
 rocks of Nova Scotia. 
 
 In Canadian Naturalist, vol. 8, 1863, p. 209, 1 
 wood-cut. 
 
 Phillipsia howi. 
 
 Description of some new species of 
 
 fossils, with remarks on others already 
 known, from the Silurian and Devonian 
 rocks of Maine. 
 
 In Proc. Portland Soc.Nat. Hist., vol. 1, 1869, 
 p. 104, plate. 
 
 Dalmanites epicrates n. s., Gheirurus tarqui- 
 nius n. s., Proetus junius n. s., P. macrobius 
 n. s., Bronteus pompilius n. s., Phaeops trajanus 
 n. s., Lichas. 
 
 Palseozoic fossils. Yol. 1. Contain- 
 ing descriptions and figures of new or 
 little known species of organic remains 
 from the Silurian rocks. 1861-’65. 426 
 pp., 401 figures. Geol. Survey Canada, i 
 
 The first portion of this work, consisting of 
 24 pages, was issued in November. 1861, and I 
 re-appears in this work, with the exception cf [ 
 the notes on pages 10, 11, and 12 of the original 
 edition. The second part, consisting of pp. ! 
 
 Billings (E.) — Continued. 
 
 25-56, was issued in January, 1862, and the 
 third, pp. 57-168, in June, 1862; the fourth, 
 pp. 169-344, in February, 1865. 
 
 Harpes, Remopleurides, Olenus, Olenellus , 
 Dolichometopus, Dikelocephalus, Telephus , Cono- 
 cephdlites, Ari&nellus, Bathyurus, Loganellus , 
 Henocephalus, Triarthrus, Harpides, Lichas, 
 Ampyx, Asaphus, Gheirurus , Sphcerexochus, 
 Amphion, Encrinurus, Illcenus, Nileus, Agnos- 
 tus, Beyrichia, Leperditia, Bathyurellus n. g., 
 Shumardia n. g.. Endymion n. g. (this name 
 was changed by the author tp that of Endy- 
 mionia on p. 281). 
 
 Catalogue of the Silurian fossils of 
 
 the island of Anticosti, with descrip- 
 tions of some new genera and species. 
 1866. 93 pp., 28 figs. Geol. Survey 
 
 Canada. 
 
 Harpes, Sphcerocoryphe, Proetus, Dalmani- 
 tes, Calymene, Lichas, Dionide, Asaphus, Chei- 
 rurus , Sphcerexochus, Encrinurus, Bronteus, 
 Illcenus, Beyrichia, Leperditia. 
 
 Note on some specimens of Lower 
 
 Silurian Trilobites. 
 
 In Quart. Jour. Geol. Soc. London, vol. 26, 
 1870, p. 479, pis. 31, 32. 
 
 Asaphus platycephalus Stokes, with some of 
 the legs preserved. 
 
 Palaeozoic fossils. Yol. 2, pt. 1. 
 
 1874. 
 
 In Geol. Survey Canada, 144 pp., 35 figs, and 
 9 pis. 
 
 Paradoxides, Anopolenus, Agraulos, Soleno 
 pleura. 
 
 On some new or little known fossils 
 
 from the Silurian and Devonian rocks 
 of Canada. 
 
 In Canadian Naturalist, new series, vol. 7, 
 1874, p. 230. 
 
 Lichas superbus n. s. 
 
 Blumenbach (J. F.) Abbildungen na- 
 turhistorischer Gegenstande. Gottin- 
 gen, 1810. 
 
 The author remarks on a species of Calymene 
 blumenbachii, which he figures on pi. 50, that 
 “according to all analogy it must have been 
 without doubt the petrifaction of some species 
 of insect without wings.” 
 
 The specimen was from Dudley limestone 
 and afterwards named by Alex. Bronguiart 
 Calymene blumenbachii. 
 
 Boeck (C.) Notitzer til Laeren om Tri- 
 lobiten. . (*) 
 
 In Nyt Mag. Naturvid., vol. 1, Christiania, 
 1827, p. 11. 
 
 Trilobitem tesseni, T. spinosus major, T. 
 spinosus minor, T. gracilis, T. zippei, T. haus - 
 manni. 
 
 Noticed in Bull. Sci. Nat. (Ferussac), vol. 
 14, 1828, p. 45. 
 
VOGDES.] 
 
 LIST OF AUTHORS. 
 
 19 
 
 Boeck (C.) — Continued. 
 
 Uebersicht der bisber in Norwegen 
 
 gefundenen Formen der Trilobiten- Fa 
 milie. (*) 
 
 In Gaea Norwegica (Keilliau), Christiania, 
 1838, pt. 1, p. 138. 
 
 Trilobiten elliptifrons , T. elegans , T. haus- 
 manni . T. semilunaris , T. punctatus, T. sphce- 
 ricus, T. clavifrons, T. blumenbachii , T. fischeri, 
 T. forficula, T. acicularis, T. lyra , T. grandis, T. 
 angustifrons, T. dilatatus, T. expansus, T. acu- 
 munatus, T. limbatus , T. striatus, T. f rontalis , 
 T. crassicauda, T. centrotus, T. asellus, T. alatus, 
 T. latus, T. granulatus, T. rostratus, T. mammil- 
 latus , T. scaraboeoides. 
 
 Om Trilobiten. 
 
 In Skand. Naturf. Forhand., vol. 2, 1840, p. 
 289; Neues Jahrbuck fur Mineral., 1841, p. 724. 
 
 Boll (Ernst). Beitrag zur Kenntniss der 
 Trilobiten. 
 
 In Danker and von Meyer’s P alaeon togra p h - 
 ica, vol. 1, Cassell, 1847, p. 126. 
 
 A inpyx, Battus. 
 
 Ueber die Arten der Gattung Bey- 
 
 richia in norddeutschen Silurian-Gerol- 
 len. 
 
 In Zeitschr. deutsch. geol. Gesell., Berlin, 
 vol. 8, 1856, p. 321, 4 figs. 
 
 A communication from Herr Boll to Herr 
 Bey rich. 
 
 Beyrichia jonesi, B. spinulosa, B. 1 nans. 
 
 Die Beyricliien der norddeutschen 
 
 silurischen Gerdlle. 
 
 In Afchiv Yereins FreundeNaturg. Mecklen- 
 burg, 1862, p. 114, pi. 1. 
 
 Beyrichia. 
 
 Born ( Chev . de). Lithophilacion Bor- 
 nianum. Index fossilium quae colleget 
 in class, ac ordinis digessit. 2 vols. 
 Pragac, 1772. (*) 
 
 In Crustacea, vol. 2, p. 5. 
 
 Bornemann (J. G.) Palaeontologisckes 
 aus dem cambrischen Gebiete von Ca- 
 malgrande in Sardinien. 
 
 In Zeitschr. deutsch. geol. Gesell., Berlin, 
 1883, p. 270. 
 
 Olenellus zoppei, Conocoryphe sp.? (Olenus 
 armatu8 Meng.), lllcenus meneghini. 
 
 Bradley (Frank). Description of a new 
 Trilobite from the Potsdam sandstone, 
 with a note by E. Billings, of Montreal, 
 CaDada. 
 
 In Proc. Am. Assoc. Adv. Sci., 14th meeting 
 1861, p. 161, 3 wood-cuts. 
 
 • Oonocephalit.es minutus. 
 
 See, also, Am. Jour. Sci., 2d series, vol. 30, 
 1860. p. 241; Canadian Naturalist, vol. 5, 1860, 
 p. 420. 
 
 Brady (M. P.) See Jones (T. Rupert), 
 Kirkby (J. W.) and Brady (M. P.). 
 
 Brocchi (M. P. ) Note sur un crustacd 
 fossile recueilli dans les schistes d’Au- 
 tun. 
 
 In Bull. Soc. G6ol. France, 3d series, vol. 8, 
 No. 1, 1880, p. 3, pi. 1. 
 
 Paloeocaris, Gampsonyx, Nectotelson n. g. 
 
 Brodie (P. B.) History of fossil insects 
 in the Secondary rocks of England. 
 London, 1845, pp. 105-115, pi. 1, fig. 11. 
 
 This author describes and figures a fossil 
 from Coalbrookdale resembling the caterpillar 
 of the Emperor moth, which was afterwards 
 described by J. W. Salter under the name of 
 Eurypterus {Arthropleura) ferox. 
 
 Brogger (W. C.) Fossiler fra Oxna og 
 Kletten. (*) 
 
 In Geol. Foreningens Stockholm Fbrhandl., 
 vol. 2, 1875, 1 pi. 
 
 Paradoxides, Liostracus, Agnostu ®. 
 
 Andrumkalk ved Breidengen val- 
 
 ders. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 3, 1876, 1 pi. 
 
 Paradoxides, Liostracus, Selenopleura, Ag- 
 nostus. 
 
 Om Trondhjemsfeldtets midlere 
 
 Afdeling mellem Guldalen og Meldalen 
 Christiania. (*) 
 
 In Vidensk. Selskab. Forhandl., 1877, No. 2, 
 p. 1, 2 pis. 
 
 Dalmanites , Trinucleus. 
 
 Om Paradoxides skifrene ved.Krek- 
 
 ling. (*) 
 
 In Nyt Mag. Naturvid., vol. 24, pt. 1, 1878, 
 6 pis. 
 
 Paradoxides, Olenellus, Dolichometopus, Lio- 
 stracus, Conocoryphe, Inomocare, Elyx, Soleno- 
 pleura, Ellipsocephalus, Arionellus, Agnostus. 
 
 Die silurischen Etagen 2 und 3 im 
 
 Kristianiagebiet und auf Eker. Kristi- 
 ania, 1882, 12 pis. 
 
 Remopleurides, Dicelocephalus, Olenus, Para- 
 bolina, Peltura, Cyclognathus, Ceratopyge, 
 Ctenopyge, Protopleura (new subgenus to the 
 genus Peltura ), Parabolinella (new subgenus 
 to the g'mus Olenus), Leptoplastus, Sphceroph - 
 tlialmus, Eurycare, Bceckia n. g., Triarthrus, 
 Euloma, Holometopus, Harpides, Phacops, 
 Lichas, Trinucleus, Ampyx, Asaphus, Mega- 
 laspis, Symphysurus, Niobe, Ptychopyge, Nileus, 
 Oheirurus, lllcenus, Dysplanus, Amphion, 
 Gybele, Agnostus, Oonophrys, Beyrichia, Leper - 
 ditia, l8ochilina. 
 
 Paradoxides olandicus nivaet ved 
 
 Ringsaker, Norge. (*) 
 
 In Geol. Foreningens Stockholm. Forhandl, 
 vol. 6, 1884, 1 pi. 
 
20 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Brogger (W. C.) — Continued. 
 
 Om aldern af Olenelluszonen i Nord- 
 
 amerika. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 8, 1886, p. 182. 
 
 TJeber die Ausbildung des Hyposto- 
 
 mes bei einigen skandinavischen Asa- 
 pbiden. 
 
 In Ofversigt Kongl. Svenska Yet. -Acad. 
 Handl., vol. 11, 1886, 3 pis. 
 
 Asaphus, Isotelus, Ptychopyge, Megalaspis, 
 Megalaspides n. g., Niobe, Asaphellus, Ogygia, 
 Nileus, Symphysurus. 
 
 Bromell (M.) Lithographia Suecana. 
 
 In Acta Literaria Suecise, vol. 2, TJpsalise, 
 1725, p. 63. 
 
 This work was continued in several parts 
 through this volume, hut it is only at p. 493, 
 in the section called “De lapidibus insectiferis 
 Scanices et Gothicis,” that the Trilobites are 
 treated. We have there the Oleni of the alum 
 slate and Agnostus pisiformis. 
 
 A separate edition of the work was printed 
 at Stockholm and Leipzig, in 1740, hearing the 
 same title as the original work. 
 
 Brongniart (Alex.) Histoire naturelle 
 des Crnstiac^s fossiles sous les rapports 
 zoologique et g^ologique, savoir les 
 Trilobites. Les Crustac^s proprement 
 dits par A.-G. Desmarest. 11 pis. 
 Paris, 1822. 
 
 This author was the first systematic writer 
 upon the Trilobites. He arranges twenty-two 
 species under five new generic names, as fol- 
 lows : First genus, Galymene, species 1. G. de 
 Blumenbach, 2. C. de Tristan, 3. G. ? variolaire, 
 4. G. ? macrophtalme. Second genus, Asaphus, 
 species 1. A.? cornigere, 2. A. de Debuch, 4. 
 A. caudigere, 5. A. large queue. Third genus, 
 Ogygia, species 1. O. de Guettard, 2. O. de 
 Desmarest. Fourth genus, Paradoxides, spe- 
 cies l.P.de Tessin, 2. P. spinuleux, 3. P. scar a- 
 bo'ide, 4. P. ? gibbeux, 5. P. lacinie. Esp&ces de 
 genre incertain : Trilobite granule, T. ponctue, 
 T. bucephale, T. tentacule. Fifth genus, Ag- 
 nostus, species 1. A. pisiforme. 
 
 - and Desmarest (A.-G.) Histoire 
 
 naturelle des Trilobites et des Crustac^s 
 fossiles. 
 
 In Jour. Mines, vol. 9, 1822, p. 273. 
 
 Bronn (Heinrich). Ueber zwei neue Tri- 
 lobiten-Arten. 
 
 In Zeitschr. fur Mineral., vol. 1, pt. 1, 1825, p. 
 317, pi. 2. 
 
 Galymene latifrons, G. schlotheimi. 
 
 Geognostische zoologische Unter- 
 
 suchungen in den russisch-baltischen 
 Provinzen von Herrn Dr. Eduard Eich- 
 wald. 
 
 In Zeitschr. fur Mineral., vol. for 1828, pt. 1, 
 p. 104. 
 
 Bronn (H. G.) Lethsea geognostica, oder 
 Abbildungen and Beschreibungen der 
 fur die Gebirgs-Formationen bezeich- 
 nendsten Yersteinerungen. Stuttgart, 
 1835-’38. 
 
 2 vols., and atlas with 47 pis. 
 
 and Roemer (F.) H. G. Bronn’s 
 
 Lethaea geognostica, oder Abbildungen 
 und Beschreibungen der fur die Gebirgs- 
 Formationen bezeichnendsten Yerstei- 
 nerungen. 3d ed. Stuttgart, 1851-’56. 
 
 3 vols. and atlas, 124 pis. ; vol. 1, p. 525. 
 
 Harpes, Harpides, Remopleurides, Paradoxi- 
 des, Hydrocephalus f Sao, Arionellus, Ellipso- 
 cephalus, Olenus , Gonocephalites, Proetus, Gy- 
 phaspis, Phillipsia, Arethusina, Phacops, Dal- 
 mania, Cryphceus, Galymene , Homalonotus, 
 Lichas, Trinucleus, Ampyx, Dionide, Asaphus, 
 Ogygia, JEglina, lllcenvs, Addas pis, Ceraurus, 
 Placoparia, Splicer exochus, Staurocephalus, Dei- 
 phon, Dindymene, Zetheis, Amphion, Enerinu- 
 rus, Cromus, Bronteus, Telephus, Agnostus, Eu- 
 rypterus, Himantopterus, Pterygotus, Limulus, 
 Gampsonychus , Cythere, Bairdia, Cypridina, 
 Cyprella, Entomoconchus, Beyrichia, Dithyro- 
 caris, Ceratiocaris. 
 
 Note iiber die mit Homalonotus ver- 
 
 wandten Trilobitengenera. 
 
 In Neues Jahrbuch fur Mineral., 1840, p. 445, 
 pi. 8, figs. 1 a, o. 
 
 Index palseontologicus, oder Ueber- 
 
 sicht der bis jetzt bekannten fossilen 
 Organismen, unter Mitwirkung der 
 HH. H. R. Goppert und Herm. von 
 Meyer bearbeitet von Dr. H. G. Bronn, 
 Nomenclator palseontologicus in alpha- 
 betischer Ordnung. Stuttgart, 1848, 
 3 vols. 
 
 Ueber Gampsonyx Jimbricatus Jordon 
 
 aus der Steinkohlen - Formation von 
 Saarbriicken und vom Murg-Thal. 
 
 In Neues Jahrbuch fur Mineral., 1850, p. 575. 
 
 Briickmann (F. E.) Epistolarum itine- 
 rariarum centuria. Wolfenbiittelse, 3 
 vols. 
 
 In Epist. 23, pi. 2, figs. 1-7, 1732, and Epist. 64, 
 pi. 3, fig. 5, 1737. 
 
 This author compares the fossil Crustacea 
 with the Mollusca and calls them Armata 
 veneris. 
 
 Brunnich (M. T. ) Beskrivelse over Trilo- 
 biten,en Dyrestagt og dens Arter, med 
 en ny Aftegning. 
 
 In Nye Samling of detKongelige Danske Yi, 
 denskabers Selskabs Skriften, Kiobenhavn- 
 1781, p. 384. 1 pi. 
 
 This author describes Trilobus ( Galymene ) 
 tuberculatus, Trilobus \Dalmanites) caudatus 
 (figures of head and pygidiura), Trilolus dilctr 
 tatus, Trilobus ( Encrinurus ) punctatus. 
 
WJGDES.] 
 
 LIST OF AUTHORS. 
 
 21 
 
 Such (Leopolu von). Beitrage zur Be- 
 stimmung der Gebirgs-Formationen in 
 Russian d. 
 
 In Archiv mineral. Geogn., etc., vol. 15, Ber- 
 lin, 1841, p. 1, pi. 2. 
 
 Phacops, Oalymene, Asaphus, Illcenus. 
 
 Buckland ( William ). Geology and 
 mineralogy considered with reference 
 to natural theology. Bridgewater trea- 
 tise. 2 vols. London, 1837, 87 pis. 
 [4th ed., London, 1869, 2 vols., 90 pis.] 
 
 Translated into German by L. A gassiz. 
 
 Paradoxides , Phillipsia, Phacops, Calymene, 
 Asaphus, Ogygia, Encrinurus, Limulus (Beli- 
 nuru8) trilobitoides. 
 
 Burmeister (H ) Die Organisation der 
 Trilob iten, etc. Berlin, 1843, 6 pis. 
 
 The English translation is entitled: “The 
 organization of Trilobites deduced from their 
 living affinities, with a systematic review of the 
 species hitherto described, by Hermann Bur- 
 meister, edited from the German by Prof* 
 Thomas Bell, E. R. S., and Prof. E. F. Forbes, 
 F. R. S.” London, Ray Society, 1846 There is 
 a supplementary appendix by the editors. 
 
 Burmeister classifies 63 species under 23 
 genera arranged in the following order : 
 
 Eurypterus, Cytkerina, Trinucleus , Ogygia , 
 Odontopleura, Arges, Bronteus , Paradoxides , 
 Olenus , Conocephalus, Ellipsocephalus. Earpes , 
 Calymene, Homalonotus, Phacops, Cyphaspis 
 n. g., Proetus, ASonia n. g., Archegonus n. g., 
 Illcenus, Dysplanus n. g M Asaphus, Ampyx. 
 
 The supplementary appendix by Thomas 
 Bell and E. F. Forbes contains an alphabetical 
 list of British Trilobites, also a copy of McCoy’s 
 generic description of the following genera: 
 Tiresia, Forbesia, Portlockia, Trinodus (Synop- 
 sis Silurian Fossils Ireland, 1846) ; the generic 
 descriptions of Cheirurus , Sphcerexochus , 
 Eichas, Trochurus (Beyrich, Ueber einige boh- 
 mische Trilobiten, 1845), and a list of the genera 
 and species described by Barrande (Notice pr6- 
 liminaire sur le syst^me silurien et les Trilo- 
 bites de Boh6me, 1846). 
 
 and Alton (Ed. de). Neue Beo- 
 
 bachtungen Uber die Organisation der 
 Trilobiten. (*) 
 
 In Zeitungfur Zoologie, Zootomie und Palaio- 
 zoologie, Alton und Burmeister, Leipzig, vol. 
 1, 1848, p. 67, pi. 1, figs. 13-19. 
 
 Callaway (Charles). On a new area of 
 Upper Cambrian rocks in South Shrop- 
 shire, with a description of a new fauna. 
 
 In Quart. Jour. GeoL Soc. London, vol. 33, 
 1877, p. 652, plate. 
 
 Olenus, Gonocoryphe, Asaphus, Asaphellus 
 (new subgenus), Platypeltes (new subgeuus), 
 Lichapyge n. g., Agnostus, Conophrys n. g. 
 
 Castelnau (Laport de). Communique h 
 PAcaddmie des sciences de Paris la d6- 
 
 Castelnau (Laport de) — Continued, 
 couverte des pieds des Trilobites qu’il 
 aurait vus dans l’int6rieur d’un exeui- 
 plaire enroul6 de PAmfhique du Nord. 
 
 In Inst. France, 1842, p. 74 ; Neues Jahrbuch 
 fur Mineral., 1843, p. 504; Comptes Rendus, 
 vol. 14, 1842, p. 344. 
 
 Calymene. 
 
 Essai sur le syst&me silurien de 
 
 PAmdrique Septentrionale. Paris, 1843, 
 27 pis. 
 
 Asaphus micrurus, A. limulurus, A. cordieri, 
 A. caudatus, A. edwardii, A. murchisoni, Ho- 
 malonotus giganteus, II. herculaneus, H. atlas, 
 Arctinurus n. g., A. boltoni, Calymene bufo, 
 Odontocephalus, Acantholoma, Aspidolites, Dis- 
 cranurus. 
 
 Champernowne (A.) Note on a find of 
 Homalonotus in Red Beds at Torquay. 
 
 In Geol. Mag., new series, decade 2, vol. 8, 
 1881, p. 487. 
 
 Chapman (E. J.) Asaphus canadensis. 
 
 In Canadian Jour., new series, vol. 1, 1856, 
 p. 482. 
 
 A review of the Trilobites, their 
 
 characters and classification. 
 
 In Canadian Jour., new series, vol. 1, 1856, p. 
 271, wood-cuts. 
 
 Trinucleus concentricus. 
 
 Iu Canadian Jour., new series, vol. 3, 1858, 
 p. 414, wood-cut. 
 
 On some new Trilobites from Cana- 
 dian rocks. 
 
 In Annals Mag. Nat. Hist., 3d series, vol„2, 
 1858, p. 9, 2 figs. 
 
 Asaphus canadensis, A. halli. 
 
 On some new Trilobites from Cana- 
 dian rocks. 
 
 In Canadian Jour., new series, vol. 3, 1858, p. 
 230, 2 wood-cuts. 
 
 Asaphus canadensis, A. halli. 
 
 On the hypostoma of Asaphus cana- 
 densis and on a third new species of 
 Asaphus from the Canadian rocks. 
 
 In Canadian Jour., new series, vol. 4, 1859, 
 p. 1, 2 figs. 
 
 Asaphus canadensis, A. hincksii. 
 
 On the probable nature of the sup- 
 posed fossil tracks known as Protich- 
 nites , etc. 
 
 In Canadian Jour., new series, vol. 16, 1877, 
 p.7. 
 
 Clarke (J. M.) New Pliyllopod Crusta- 
 ceans from the Devonian of western 
 New York. 
 
 In Am. Jour. Sci., 3d series, vol. 23, 1882, p. 
 476, plate. 
 
 Estheria, Spathiocaris n. g., Lisgocaris n. g. 
 
[BULL. 63. 
 
 22 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Clarke (J. M.)— Continued. 
 
 Girriped Crustacean from the De- 
 vonian. 
 
 In Am . J our. Sci., 3d series, vol. 24, 1882, p. 55. 
 
 Plumulites devonicus. 
 
 New discoveries in Devonian Crus- 
 tacea. 
 
 In Am. Jour. Sci., 3d series, vol. 25, 1883, p. 
 
 120 . 
 
 Dipterocaris n. g. 
 
 Ueber deutsclie oberdevonische 
 
 Crustaceen (hierzu) Tafel 4. 
 
 In Neues Jalirbuch fur Mineral., 1884, pt. 1, 
 p. 178. 
 
 Spathiocaris, Entomis, Dithyrocaris. 
 
 On the higher Devonian fauna of 
 
 Ontario County, New York. 
 
 In Bull. U. S. Geol. Survey, No. 16, 1885, 3 pis. 
 
 Ceratiocaris, Beyrichia, Echinocaris, Spathio- 
 caris. 
 
 The structure and development of 
 
 the visual area in the Trilobite Phacops 
 rana Green. 
 
 In Jour. Morphology, vol. 2, No. 2, Nov., 1888, 
 Boston, p if 253, pi. 21. 
 
 Clarke (W. B.) On the occurrence of 
 Trilobites in New South Wales. 
 
 In Quart. Jour. Geol. Soc. London, vol. 4, 1848, 
 p. 63 (not descriptive). 
 
 Claypole (E. W.) Note on a large Crus- 
 tacean from the Catskill group of 
 Pennsylvania. 
 
 In Proc. Am. Philos. Soc., Phila., vol. 21, 1883, 
 p. 236, plate. 
 
 Dolichocephala n. g. 
 
 On the occurrence of the genus Dal- 
 
 manites in the Lower Carboniferous 
 rocks of Ohio. 
 
 In Geol. Mag., decade 3, vol. 1, London, 1884, 
 p. 303. 
 
 Dalmanites? cuyahogce. 
 
 Conrad (T. A. ) Report on the Palaeonto- 
 logical Department. 
 
 In Kept. Geol. Survey New York, 1838, p. 107. 
 
 Platynotus n. g. 
 
 On the Silurian system ; with a table 
 
 of the strata and characteristic fossils. 
 
 In Am. Jour. Sci., 1st series, v<Jl. 38, 1840, p. 86. 
 
 Third Anuual Report on the Palae- 
 ontological Department of the Survey. 
 
 In Kept. Geol. Survey New York, 1840, p. 199. 
 
 Odontocephalus n. g., Acanihaloma n. g., 
 Odontocephalus selenurus , Asaphus halli, 
 Acidaspis tuberculatus. 
 
 Description of new genera and spe- 
 cies of organic remains. Crustacea. 
 
 In Rept. Geol. Survey New York, 1841, p. 48, 
 
 lpl. 
 
 Conrad (T. A.) — Continued. 
 
 Aspidolites n. g., Dicranurus n. g., Asaphus ? 
 acantholeurus , A.? denticulatus , A. nasutus, 
 A. aspectans, Calymene-senaria. 
 
 The plate accompanying this report was 
 distributed with a few copies. Republished in 
 the 15th Rept. New York State Cab. Nat. Hist., 
 pi. 11. 
 
 Cytherinaalta. 
 
 In Geol. Survey New York, pt. 3, comprising 
 the survey of the 3d Geol. Dist. (Vanuxem), 
 1842, p. 112, fig. 23, No. 6. 
 
 Observations on the Silurian and 
 
 Devonian systems of the United States, 
 with descriptions of new organic re- 
 mains. 
 
 In Jour. Acad. Nat. Sci., Phila., vol. 8, 1842, p. 
 228, 6 pis. 
 
 Asaphus corycosus, A. ? trentonensis, Calymene 
 spinifera, G. earner ata, Dipleura. 
 
 Observations on the lead-bearing 
 
 limestone of Wisconsin, and descrip- 
 tions of a new genus of Trilobites and 
 fifteen new Silurian fossils. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 1, 1843, p. 
 329. 
 
 Thaleops n. g. 
 
 Corda (A. J. C.) and Hawle (Ignaz). 
 Prodrom einer Monographie der bohmi- 
 schen Trilobiten. 
 
 In Abhandl. bohm. Gesell. "Wiss., Prag, vol. 5, 
 1847, pp. 129-292, 7 pis. 
 
 This work is generally attributed to A. J. C. 
 Corda. The 58 new genera described in this 
 work are arranged by Joachim Barrande, Sys- 
 teme silurien du centre de la Boheme, vol. 1, 
 p. 39, as follows : 
 
 I. Division. Telejurides. 
 
 Phhysacium i 
 
 = Hydrocephalus Barr. 
 
 S == Sao Barr. 
 
 Phanoptes 5 
 Crithias 
 Tetracnemis 
 Goniacanthus 
 Enneacnemis 
 Acanthocnemis 
 Acanthogramma 
 Eudogramma 
 Micropyge 
 Selenosema 
 Staurogmus j 
 Herse 
 Agraulos 
 Conocoryplie 1 
 
 Ptychoparia )• = Conocephalus Zenk. 
 Ctenocephalus. j 
 Selonopeltis= Acidaspis Murch. 
 Polytomurus = Dionide Barr. 
 Tetrapsellium — Trinucleus Lhwyd. 
 Phalacroma= Agnostus (in part) Brong. 
 Selenoptyclius = iEglina Barr. 
 Mesospheniscus = Agnostus integer Beyr. 
 Diplorrhina = Agnostus integer. 
 
 | = Arionellus 
 
 Barr. 
 
VOGDES.] 
 
 LIST OF AUTHORS. 
 
 23 
 
 Corda (A. J. C.) and Hawle (Ignaz) — 
 Continued. 
 
 I. Division. Telejurides— C ont’d. 
 
 25. Condylopyge ) _ ^g nog ^ us rex B arr . 
 
 26. Lejopyge 3 
 
 27. Microparia = JEglina Barr. 
 
 28. Pl8esiacomia = I]l8enu3 Dalm. 
 
 29. Cyclopvge=iEglina (in part) Barr. 
 
 30. Alceste = Illaenus (in part) Dalm. 
 
 31 Xiphogonium = Proetus Stein. 
 
 32. Conoparia = Cyphaspis Burin. 
 
 33. Goniopleura — Proetus elegantulus Ang. 
 
 34. Aulacopleura = Arethusina Barr. 
 
 35. Pharostoma = Calymene Brong. 
 
 ^ ra ® to PJ se ^ = Dalmania (in part) Emmrkh. 
 37. Odontoeliile 3 ^ 
 
 (This generic term was used in 1834 for a genus 
 of the Coleoptera). 
 
 II. Division. Odonturides. 
 
 38. Amphytrion ==Remopleurides Portlock. 
 
 39. Artlirorhachis = Agnostus tardus Barr. 
 
 40. Peronopsis = Agnostus integer Beyr. 
 
 41. Battus = Agnostus integer. 
 
 42. Pleuroctenium‘= Agnostus granulatus Barr. 
 
 43. Thysanopeltis = Bronteus (in part) Gold. 
 
 44. Dind>mene = Bindymene Corda. 
 
 , „ . . . c Proetus (in part) Stein. 
 
 45. Pnonopelt.s= ptiEtoIliae3 Barr . 
 
 46. 
 
 47. 
 
 48. 
 
 50. 
 
 51. 
 
 52. 
 
 53. 
 
 54. 
 
 56. 
 
 58. 
 
 Asteropyge ) __ j) a ^ man i a (} n p ar t) Dalm. 
 Metacanthus 3 
 
 Odontopyge = Olenus spinulosus. 
 Placoparia = Placoparia Corda. 
 Eccoptochile = Cheirurus Beyr. 
 Actinopeltis = Cheirurns Beyr. 
 
 Trochurus = Staurocephalus Barr. 
 Corydocophalus 
 Dicranopeltis 
 Acanthopyge 
 Dicranogmus J 
 Trapelocera = Acidaspis Murch. 
 Ceratopyge= Olenus forficnla Sars. 
 
 Cozzens (Issachar). Description of three 
 new fossils from the Falls of the Ohio. 
 
 In Annals Lyceum Nat. Hist. «New York, 
 vol. 4, 1846, p. 157, 1 pi. 
 
 Piliolites n. g. 
 
 The author therein describes a species of 
 Proetus under the name of Piliolites ohioensis. 
 
 Da Costa (E. M.) A letter concerning 
 the fossil from Dudley. 
 
 In Philos. Trans. Royal Soc., vol. 48, pt. 1, No. 
 42, 1753, p. 286, pi. 1, figs. 6-8. 
 
 Dr. Da Costa herein gives the name of Pedi- 
 cuius marimns major trilobus to the then called 
 Dudley fossils ( Calymene blumenbachii) , and 
 declares it to be a crustaceous animal nearly 
 related to the living Isopodes. 
 
 Description of a curious fossil ani- 
 
 mal. 
 
 In Gentleman’s Mag., vol. 25, London, 1754, p. 
 24, pi. — , fig. 3. 
 
 Calymene blumenbachii. 
 
 I Dalman(J.W.) N&grapetrificater fundne 
 i Ostergotlands ofvergangskalk after- 
 knade och beskrifne. 
 
 In Svenska Vetensk. Akad. Handl., 1824, p. 
 368, pi. 4. 
 
 Entomostr. actinurus. 
 
 Om Palseaderna eller de sa kallade 
 
 Trilobiterna. Stockholm, 1826, 6 pis. 
 
 Svenska Vetensk. Akad. Handl., 1826, p. 226. 
 
 The German translation bears the following 
 title: Ueber die Palseaden, oder die sogenann- 
 ten Trilobiten von J. D. Dalman, von Friedrich 
 Engelhart, mit 6 Kupfertafeln, Niirnberg, 1828. 
 
 Dalman arranges 41 species of Trilobites 
 under 5 genera and 4 subgenera, as follows : 
 
 Division I. Oculated: 1st genus, Calymene ; 
 2d genus, Asaphus. 
 
 Division II. Typhlini : 3d genus, Ogygia; 4th 
 geuus, Olenus ( Paradoxides Br.). Section 2. 
 Battoides : 5th genus, Battus (Agnostus Br.). 
 
 Subgenera: 1. Asaphus ( Nileus ); 2. Asaphus 
 (Illcenus) ; 3. Asaphus (Ampyx) ; 4. Lichas n. g. 
 
 Arsberattelse om nyare zoologiska 
 
 arbeten och upptackter. 
 
 This work forms a part of the annual report 
 of the keepers of the Swedish State Museum 
 for 1828. It contains (p. 134), under the title of 
 “Nya Svenska Palaeades” a description of the 
 following Trilobites: Calymene ornata, C. ver- 
 rucosa, C. clavifrons, C.? centrina, Asaphus 
 heros, A. platynotus, Nileus qlomerinus , Ampyx 
 pachyrrhinus, Battus Icevigatus, B. pisiformis. 
 
 Nouvelles especes de Trilobites ou 
 
 Paheades de Suede. 
 
 In Bull. Ferussac, vol. 19, 1828, p. 129. 
 
 A notice of the preceding reference. 
 
 Dames (W.) Ueber Hoplolichas und Cono- 
 lichas , zwei Untergattungen von Lichas. 
 
 In Zeitschr. Deutsch. geol. Gesell.,' Berlin, 
 1877, vol. 29, pt. 1, p.793, 3 pis. 
 
 The type used for the new genus Hoplolichas 
 is Lichas tricuspidatus Boll, and for Conolichas, 
 Lichas asquiloba Steinh. 
 
 Geologische Reisenotizen aus Schwe- 
 
 den. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 1881, vol. 33, p. 405. 
 
 Paradoxides celandicus, P. tessini, P. forch- 
 hammeri, P. kjerulfi, Ellipsocephalus , Lichas, 
 Megalaspis, Asaphus?, Agnostus. 
 
 Erste Abhandlung. Cambrische 
 
 Trilobiten von Lian Tung, China 
 (Richthofen). Vol. 4. Berlin, 1883, 
 pis. 1,2. 
 
 The author suggests the new generic term 
 Dorypyge for certain Trilobites which have the 
 pygidium armed with strong spines, thepennb 
 timate pair being the longest, including in the 
 genus Dikelocephalus quadriceps Hall and Whit- 
 field and D. gothicus Hall and Whitfield. 
 
24 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Dames (W.) — Continued. 
 
 Under Anomocare Angelin he includes the 
 following American species : Conocephalites 
 
 hamulus Owen, C. wisconsinensis Owen, and 
 C. patter soni Hall. 
 
 Conocephalites frequens, C. quadriceps , C. ty- 
 pus, C. subquadratus, Anomocare latelimbatum, 
 A. minus, A. planum, A. nanum, A. majus, A. 
 subcostatxim, Liostracus talingensis, L. megalu- 
 rus , Dorypyge n. g., D, richthofeni, Agnostus 
 chinen. 
 
 E. W. Claypole : On the occurrence 
 
 of the genus Dalraauites in the Lower 
 Carboniferous rocks of Ohio. Geol. 
 Mag. London, 1884. 
 
 In Neues Jahrbuch fur Mineral., 1885, vol. 
 1, p. 102 (abstract). 
 
 Dalmanites, Phillipsia, Proetus. 
 
 C. D. Walcott: Appendages of the 
 
 Trilobites. Science, vol. 3. 1884, p. 279. 
 
 In Neues Jahrbuch fur Mineral., vol. 1, p. 
 102 (abstract). 
 
 Asaphus , Calymene, Ceraurus. 
 
 T. R. Jones and J. W. Kirkby: On 
 
 some Carboniferous Entomostracafrom 
 Nova Scotia. Geol. Mag. London, 1884. 
 
 InNeqps Jahrbuch fur Mineral., vol. 1, 1885, 
 p. 106 (abstract). 
 
 Leperditia, Beyrichia. 
 
 T. R. Jones and H. Woodward : 
 
 Notes on Phyllopdiform Crustacea, re- 
 ferable to the genus Echinocaris from 
 the Palaeozoic rocks. Geol. Mag. Lon- 
 don, 1884. 
 
 In Neues Jahrbuch fur Mineral., vol. 1, 1884, 
 p. 110 (abstract). 
 
 Chas. E. Beecher : Ceratiocaridae 
 
 from the Chemung and Waverly group 
 of Warren County. Second Geol. Sur- 
 vey, Penn. Rept. PPP. 
 
 In Neues Jahrbuch fur Mineral., vol. 1, 1884, 
 p. 110 (abstract). 
 
 ■ J. Mickleborough : Locomotory ap- 
 
 pendages of Trilobites. Geol. Mag. 
 London, 1884. 
 
 In Neues Jahrbuch fur Mineral., 1885, p. 477. 
 
 F. Schmidt and T. R. Jones: On 
 
 some Silurian Leperditia. Annals Nat. 
 Hist., series 5, vol. 9, 1882, p. 168. 
 
 In Neues Jahrbuch fiir Mineral., 1885, vol. It 
 p. 105 (abstract). 
 
 Dana (James D. ) Trilobites in the Pots- 
 dam sandstone. 
 
 In Edinburgh New Philos. Jour., vol. 6, 1857, 
 p. 350. 
 
 On the supposed legs of Trilobites 
 
 ( Asaplius platycephalus). 
 
 In Annals Nat. Hist., 4th series, vol. 7, Lon- 
 don. 1871, p. 366; Am. Jour. Sc., 3d seiies vol. 
 1, 1871, p. 320. 
 
 Dana (James D.)— Continued. 
 
 Manual of geology, treating of the 
 
 principles of the science with special 
 reference to American geological his- 
 tory. 2d ed. New York, 1874, p. 174. 
 
 D’Archiac (A.) and Verneuil (E. de). 
 On the fossils of the older deposits in the 
 Rhenish Provinces, preceded by a gene- 
 ral survey of the fauna of the Palaeozoic 
 rocks, and followed by a tabulated list 
 of the fossils of the Devonian system of 
 Europe. 
 
 In Bull. Soc. G6ol. France, vol. 13, 1841— ’42 ; 
 Trans. Geol. Soc. Lond., vol. 6, pt. 2, 1842, p. 303. 
 
 , Fischer (de Waldheim G.) and 
 
 Verneuil (E. de). Pal&mtologie de 
 PAsie Mineure. Paris, 1866, atlas, 21 
 pis. (*) 
 
 Dawson (J. W.) On the Lower Coal 
 Measures as developed in British 
 America. 
 
 In Quart. Jour. Geol. Soc. London, vol. 15, 
 1859, p. 62. 
 
 Tracks of a Crustacean. 
 
 Note on the fossils of Nova Scotia. 
 
 In Canadian Naturalist, vol. 5, 1860. p. 297 
 (wrongly paged 197 in the volume). 
 
 Homalonotus dawsoni Hall. 
 
 On the foot prints of Limulns as com- 
 pared with the Protichnitts ol the Pots- 
 dam sandstone. 
 
 In Canadian Naturalist, vol. 7, 1862, p. 271 
 Am. Jour. Sci., 2d series, vol. 34, 1862, p. 416. 
 
 Acadian geology. The geological 
 
 structure, organic remains, and mineral 
 resources of Nova Scotia, New Bruns- 
 wick, and Prince Edward Island, etc. 
 London. 
 
 Three editions, 1855-’78 (3d ed. contains the 
 supplement to the 2d ed.). 
 
 Paradoxides , Conocephalites, Phillipsia, Dal- 
 manites, Agnostus, Microdiscus. 
 
 Mr. C. F. Hartt’s descriptions of the trilo- 
 bites first appeared in the third edition of this 
 work. The original MSS. described Micro- 
 discus dawsoni under the new generic name of 
 Dawsonia, but on Prof. E. Billings’s authority 
 the author has referred it to Microdiscus daw- 
 soni. 
 
 Eurypterus, Estheria, Leaia, Beyrichia, Le- 
 perditia, Cythere , Diplostylus. 
 
 Supplement to the 2d edition of 
 
 Acadian geology. Containing addi- 
 tional facts as to the geological struct- 
 ure, fossil remains, and mineral re- 
 sources of Nova Scotia, New Brunswick, 
 and Prince Edward Island. London, 
 
 | 1878. 
 
VOGDES.] 
 
 Dawson (J. W.) — Continued. 
 
 Homalonotua dawsoni, Protirhnites carbo- 
 narius , Anthracopalcemon ( Palceocarbus ) hil- 
 lianum. 
 
 Note on two Palaeozoic Crustaceans 
 
 from Nova Scotia. 
 
 In Geol. Mag., decade 2, vol. 4, London, 1877, 
 p. 56. (See, also, Supplement Acadian Geol., 
 1878, p. 55, fig. 10.) 
 
 Anthracopalcemon (Palceocarabus) hillianum, 
 Homalonotus dawsoni. 
 
 Day (F. H.) On the fauna of the Niagara 
 and Upper Silurian rocks as exhibited 
 in Milwaukee County, Wisconsin, and 
 in counties contiguous thereto. 
 
 In Trans. Wisconsin Acad. Sc., vol. 4, 1876- 
 *77, p. 113. 
 
 Dekay ( J. E. ) Observations on the struc- 
 ture of Trilobites, and description of an 
 apparently new genus; with notes on 
 the geology of Trenton Falls, by James 
 Renwick. Read Nov. 22 (1824). 
 
 In Annals Lyceum Nat. Hist., New York, vol. 
 1, 1824. p. 174, 2 pis. ; Isis (oder Encycl. Zeit- 
 ung), Oken, 1825 and 1832. 
 
 Isotelus n. g. 
 
 Observations on a fossil crustaceous 
 
 animal of the order Branchiopoda. 
 Read Dec. 12, 1825. 
 
 In Annals Lyceum Nat. Hist., New York, vol. 
 1, pt. 2, p. 375, pi. 29. Republished in Harlan’s 
 Med Phys. Researches, 1835, p. 297. 
 
 Eurypterus n. g. 
 
 Report on several fossil raultilocular 
 
 shells from the State of Delaware; with 
 observations on a second specimen of 
 the new fossil genus Eurypterus. Read 
 Oct. 2, 1827. 
 
 In Annals Lyceum Nat. Hist., New York, 
 vol. 2, 1828, p.273. 
 
 Deslongchamps (E.) M^moire sur les 
 corps organises fossiles du gr&s inter- 
 mddiaire du Calvados. 
 
 In Soc. Linn. Calvados, vol. 2, 1825, p. 291, 2 
 pis. 
 
 The author herein describes two species of the 
 genus Homalonotus under the names Asaphus 
 brongniarti and A. brevicaudatus. 
 
 Dethleff (von) and Boll (Ernst). Die 
 Trilobiten Mecklenburgs. 
 
 In Arcbiv Vereins Freunde Naturg. Mecklen- 
 burg, 1858, p. 155. 
 
 Remopleurides , Paradoxides, Ellipsocephalus, 
 Olenus, O. ( Sphcerophthalmu8 ), Proetus, Gyphas- 
 pis. Harpides , Phacops, Galymene, Uomalono- 
 tus, Licha8. Trinucleus. A mpyx , A saphus, Ogy- 
 gin, IUcenu8. Nileus, Acidaspis , Gheirurus, 
 Sphcerexochux, Sphcerocoryphe. Amphion, En- 
 crinurus, Bronteus , Telephus, Holometopus, Do- 
 lichometopus , Agnostus. 
 
 25 
 
 Devine (T.) Description of a uew Trilo- 
 bite from the Quebec group. 
 
 In Canadian Naturalist, vol. 8, 1863, p. 95, 2 
 figs. 
 
 Loganellus n. g. 
 
 Similar forms have been referred by Corda to 
 the genus Ptychoparia. 
 
 Description of a new Trilobite from 
 
 the Quebec group. 
 
 In Canadian Naturalist, vol. 8. 1863, p. 210, fig. 
 
 Menocephalus salteri. 
 
 Dewalque (G.) Prodrome d’une descrip- 
 tion gdologique de la Belgique. Bru- 
 xelles, 1868; 2d ed., 1880. 
 
 Contains important list of fossils, and obser- 
 vations. 
 
 Dumont (A.-H.) M<3moire sur la consti- 
 tution g^ologique de la province de 
 Liege. 
 
 In M6m. Cour. Acad. Roy. Sci., Bruxelles, 
 vol. 8, 1832, p. 353. Table of fossils. 
 
 Durocher (J.) Sur le test des Trilobites 
 et des auimaux fossils de la Bretagne 
 en general. 
 
 In Bull. Soc. G6ol. France, 2d series, vol. 7, 
 p. 307, also vol. 8, 1850-’51, p. 160. 
 
 Dwight ( W. B. ) Recent explorations 
 in the Wappinger Valley limestone of 
 Dutchess County, New York. 
 
 In Am. Jour. Sci., 3d series, vol. 27, 1884, p. 
 349, pi. 7. 
 
 Bathyurus. 
 
 Eaton (Amos). Geological Equivalents. 
 
 Description of Ogygies latissimus and Gancer 
 trilobioides. 
 
 In Am. Jour. Sci., 1st series, vol. 21, 1832, pp. 
 135, 136, note. 
 
 Gancer trilobioides , Oxygies. 
 
 Trilobites. 
 
 Am. Jour. Sci., 1st series, vol. 22, 1832, p. 165. 
 
 Brongniartia n. g. 
 
 We learn from reference to Dr. Amos Eaton’s 
 description and figures given in his “Geological 
 text-book,” p. 33, pi. 1, fig. 3 (2d ed., 1832), that 
 the original of Brongniartia carcinodea Eaton 
 was the same as that afterwards described by 
 Dr. Jacob Green (Monthly Am. Jour Geology, 
 vol. 1, June, 1832; also Mon. Tril. N. A., p. 87, 
 pi. 1, fig. 6, cast 34) as Triarthrus beckii. 
 
 Geological text-book for aiding the 
 
 study of North American geology ; be- 
 ing a systematic arrangement of facts 
 collected by the author for his pupils, 
 etc. 2d ed., 5 pis. (June 15, 1832). 
 
 The following species are described in this 
 work, pp. 31-34: Genus Galamena, G. blumen- 
 bachii (Galymene smaria Conrad), pi. 2, fig. 19; 
 genus Asaphus, A. hansmannii , A. caudatus 
 (Dalmanites limulurus Green), pi. 2, fig. 18; A. 
 selenourus (Dalmanites selenurus Eaton), pi. 1, 
 
 LIST OF AUTHORS. 
 

 26 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Eaton (Amos) — Continued, 
 fig. 1 ; genus Brongniartia, B. platycephala 
 ( Homalonotus dekayi Green), pi. 2, fis, 20 ; B. 
 isotelea (Asaphus platycephalus Stokes), pi. 2, 
 fig. 22; B. carcinodia ( Triarthrus becki Green), 
 pi. 1, fig. 3; genus Nuttainiu , N. concentrica 
 (Trinucleus concentrica Eaton), pi. 1, fig. 2 ; N. 
 sparsa (Homalonotus dekayi Green). 
 
 Eichwald (Eduard). Observationes gp- 
 ognostico-zoologicse perlugriam maris- 
 que Baltici Provincias nec non de Trilo- 
 bites. Casani, 1825, 4 pis. 
 
 The author herein describes and figures eight 
 species of Lower Silurian Trilobites under the 
 new generic term Cryptonymus. In his later 
 work (“Lethoea Eossica,” p. 1449) the first three 
 are referred to the genus Asaphus ; viz, Crypto- 
 nymus schlotheimii to Asaphus schlotheimii, 
 Cryp. weissii to Asaphus weissii, Cryp.panderi j 
 to Asaphus expansus Wahl. The last five are [ 
 classed as follows : Cryp. lichtensteinii under I 
 Niobe lichtensteinii , Cryp. rosenbergii to Illcenus 
 rosenbergii , Cryp. wahlenbergii to Illcenus wah- 
 lenbergii , Cryp. rudolphii to Illcenus rudolphii , 
 Cryp. parkinsonii to Illcenus parkinsonii. 
 
 This work also contains a description and a 
 figure of Asaphus fischeri (Amphi'on fischeri 
 Eieh*). 
 
 The description of two new Carbonic Trilo- j 
 bites are added by Dr. G. Fischer, pp. 53-55, pi. 
 
 4, figs. 4 and 5, Asaphus brongniarti, pi. 4, fig. 5. 
 and A. eichwaldi, pi. 4, fig. 4. Yalerian von i 
 Moller ( 1 ‘ Ueber die Trilobiten der Steinkohlen- j 
 formation des Ural,” 1867, p. 7) refers these 
 species to Phillipsia eichwaldi Fisch., applying 
 the term to the non-mucronate pygidium. The 
 Russianmucronate species, figured by Eichwald 
 (“Lethoea Eossica,” pi. 54, fig. 10) as Griffith! \ 
 des eichwaldi , was assigned by the same author 
 to Phillipsia mucronata McCoy. 
 
 Zoologia specialis, quam expositis 
 
 animalibus turn vivis turn fossibilibus 
 postissernum Rossise in Universum et j 
 Polonise. Vilna?, vols. 1-3, 1829-’31. (*) | 
 
 Die Tbier- und Pflanzenreste des al- 
 
 ten rothen Sandsteins und Bergkalk in 
 Novgorodiscben Gouvernement. 
 
 In Bull. Acad. Petropol. St. Petersburg, vol. 
 
 7, 1840, p. 78. 
 
 Otarion eichwaldi. 
 
 Ueber das silurische Scbicbten-Sys- 
 
 tem von Ehstland. St. Petersburg, 
 1840. 
 
 Krustazeen, p. 64. 
 
 Calymene odini, O. blumenbachii Brong., C. 
 downingia Murch., C. macrophthalma Murch., 
 
 C. bellatula Dalm . , C. sembnitzkii, Amphion ( Asa- 
 phus) fischeri, Zethus verrucosus Pander, Cryp- 
 tonymus punctatus (Wahl.) Eichwald, C.vario- 
 laris, C. worthii , Asaphus expansus Wahl., A. 
 weissii, A. schlotheimii, A latus Pander, A. la- 
 ceniatus Dalm., A. dilatatus Dalm., A. devexus, 
 
 Eichwald (Eduard)— Continued. 
 
 A. tyrannus Murch., A.vulcani Murch., Illcenus 
 crassicauda Dalm., I. rosenbergii , I. coinutus 
 Pander, I.perovatis Murch., I.centrotus Dalm., 
 Trinucleus sparskii. Homalonotus herschelii 
 Murch., Nileus armadillo Dalm., Agnostus na- 
 sutus Dalm. 
 
 Die Ur welt Russlands durck Abbild- 
 
 ungen erlautert. 
 
 4 pts., St. Petersburg, 1840-’48, 14 pis. 
 
 In the first part of this work, in the list of 
 fossils given, p. 22, Eduard von Eichwald re- 
 fers three species to Cryptonymus ; a generic 
 name which he used in 1825 for an entirely dif- 
 ferent series of fossil Crustacea. In t he present 
 work ho substitutes the name for such species 
 as Calymene variolaris, C. punctatus, C.worthi, 
 etc. The name is used without a generic de- 
 scription, and only indicated by the above 
 named species. 
 
 Metopias n. g., pt. 2, p. 64, pi. 3, fig. 4. 
 
 Beitrage zur Geologie und Palajon- • 
 
 tologie Russlands. Moscau, 1854. 
 
 Bunodes n. g. 
 
 Die Grauwacken Schichten von Liv- - 
 
 und Estland. 
 
 In Bull. Soc. Imp. des Xaturalistes Moscou, 
 vol. 27, 1854, no. 1, p. 3. 
 
 Eurypterus , Pterygotus, Bunodes, Sphagodus .? 
 Ueber die Gattungen Cryptonymus 
 und Zethus. 
 
 In Bull. Soc. Imp. des Naturalistes Moscou, 
 vol. 28, 1855. Separate ed., Moscou, 1855, 23 pp. 
 
 The author maintains that the genus Cryp- 
 tonymus should be retained for several Russian 
 and Swedish Trilobites as defined by N. P. 
 Angelin (“Palaeont. Scand.,” 1852, p. 2), with 
 Calymene punctatus as its type. 
 
 Beitrage zur geographiseben Yer- 
 
 breitung der fossilen Tbiere Russland’s. ■ : 
 
 In Bull. Soc. Nat., Moscou, vols. 28-30,1855- 
 ’57 (vol. 30, 1857). 
 
 Harpes, Proetus, Cyphaspis, Homalonotus, I 
 Calymene, Griffithides, Phacops, Chasm ops, Odon- 
 tochile, Lichas, Trinucleus , Ampyx, Asaphus, ~ 
 Ptychopyge, Megalaspis, Nileus, Illcenus, Dys- 
 planus, Cheirurus, Sphcerexochus, Amphion, 
 Cryptonymus , Bronteus, Loncliodomas, Itaphia V 
 phorus , Zethus, Sphcerocoryphe, Eurypterus, 
 Pterygotus , Beyrichia, Bairdia. 
 
 Letboea Rossica, ou pal(;ontologie de 
 
 la Russ. Stuttgart, 1852- , 69. 3 vols., j 
 
 with atlas, 113 pis. 
 
 The Crustacea are arranged in the following 
 order: First order, Ostracopouia, first family,-*, 
 Cypridina, genus 1. Leperditia, 2. Bairdia, 3. ~ 
 Bexjrichia. Second order, Poecilopoda, second ; 
 family, Agnostidae, genus 4. Agnostus. Third 
 order, Copepoda, ! third family, Eurypterid®, , 
 genus 5. Eurypterus , 6. Pterygotus. Fourth \ 
 order, Xiphosurid®, fourth family, Limulid®, 
 genus 7. Campylocephalus n. g. Fifth order, 
 Isopodes, Trilobites, family Harpid®, genus 9. 
 
 
VOGDES. ] 
 
 LIST OF AUTHORS. 
 
 27 
 
 Eichwald (Eduard*)— Continued. 
 
 Harpes, 10. Trinucleus, 11. Ampyx, 12. Loncho- 
 domas, 13. Raphiophorus ; sixth family, Lick i- 
 % dae, genus 14. Licltas ; seventh family, Chei- 
 ruridae, genus 15. Acidaspis, 16. Ceraurus, 17. 
 
 ; Sphcerexochus, 18. Zethus, 19. Sphcerexocoryphe ; 
 eighth family, Amphionidae, genus 20. Aviphion, 
 21 . Romalonotus,22. CryptQnymus ; ninth family, 
 Calyminidae, geuus 23. Calymene, 24. Acaste, 25. 
 Phacops, 26. Chasmops, 27. Proetus, 28. Griffi- 
 thides, 29. (not given), ZQ.Cyphasis; tenth lamily, 
 Kemopleuridae, genus 31. Bunodes, 32. Pseu- 
 u doniscus, 33. Remopleurides ; eleventh family, 
 Asaphidae, geuus 34. Asaphus, 35. Megalaspis, 
 36. Niobe, 37. Ptychopyge, 38. Ogygia, 39. Illcenus , 
 40. Rhodope , 41. Dysplanus , 42. Actinobolus, 43. 
 Nileus; twelfth family, Brontid®, genus 44. 
 Bronteus. 
 
 . Beitrage zur nahern Ivenntniss der 
 
 in meiner Lethaea Rossica beschrie- 
 ! benen Illaenus, etc. 
 
 In Bull. Soc. Imp. des Naturalistes Moscou, 
 
 ' 1863, No. 4, p. 372. 
 
 J v Nileus , Bumastus. 
 
 Emerson (B. K.) On the geology of 
 Frobisher Bay and Field Bay. 
 
 Appendix 3. Narrative of the second Arctic 
 expedition made by Charles F. Hall, 45th Cong., 
 3d sess., Senate Doc. 27, Washington, 1879. 
 
 Triarthrus, Cyphaspis, Phacops, Calymene, 
 Asaphus, Beyrichia, Leper ditia, Primitia. 
 
 Emmons (Ebenezer). Geology of New 
 York. Pt. 2. Comprising the survey of 
 the Second Geological District. Al- 
 bany, 1842. 
 
 Isotelus gigas, fig. 99 (1) ; Bumastus trenton- 
 ensis, fig. 100 (1) ; Calymene senaria, fig. 100 (2) ; 
 Illcenus trentonensis, fig. 100 (3); Ceraurus 
 pleurexanthus , fig. 100 (6); Trinucleus tessellatus, 
 fig. 100 (7) ; Triarthrus beckii, fig. 110 (1) ; Tri- 
 nucleus caractaci, fig. 112 (1). 
 
 The Taconic system, based on ob- 
 servations in New York, Massachusetts, 
 Maine, Vermont, and Rhode Island. 
 Albany, 1844, 6 pis. and map. 
 
 Atops trilineatus n. s. and genus, fig. 8 ; Ellip- 
 tocepala asaphoides n. s. and genus (not Ellip - 
 socephalus Zenker, 1833), fig. 9. 
 
 Agriculture of New York, comprising 
 
 an account of the classification, com- 
 position, and distribution of tho soils 
 and rocks, etc. Vol. 1. Albany, 1846, 
 21 pis. and maps. 
 
 Atops trilineatus, fig. 8; Elliptocephala asa- 
 phoides, fig. 9. 
 
 On the identity of the Atops trili- 
 neatus and the Triarthrus beckii Green, 
 with remarks upon the Elliptoccphalus 
 
 asaphoides. 
 
 Emmons (Ebenezer)— Continued. 
 
 In Proc. Am. Assoc. Adv. Sci., First meet- 
 ing. Philadelphia, 1848. 
 
 Atops trilineatus, Triarthrus beckii, Elipto- 
 cephalus asaphoides. 
 
 American geology, containing a 
 
 statement of the principles of the sci- 
 ence, with full illustrations of the char- 
 acteristic fossils. Vol. 1, Parts I, II, 
 and III. Albany, 1855-57, atlas, 17 pis. 
 
 Dikelocephalus, Olenus, Triarthrus, Atops, 
 Conocephalus, Elliptocephdlus , Phacops, Caly- 
 mene, Trinucleus, Isotelus, Ogygia, Illcenus, 
 Acidaspis, Ceraurus, Agnostus, Microdiscus n. 
 g., Beyrichia, Cytherina, Cyproides. 
 
 Manual of geology, designed for the 
 
 use of colleges and academies. New 
 'York, 1860. 
 
 Paradoxides? quadrispinosus , fig. 57; Para- 
 doxides macrocephalus, fig. 70 ; Atops punctatus, 
 fig. 71; Microdiscus quadrico status, fig. 73; 
 Calymene senaria, fig. 87 ; Illcenus trentonensis, 
 fig. 89 (a); Illcenus crassicauda, fig. 89 (b); Tri- 
 arthrus beckii, figs. 89 (c) and 91 ; Isotelus gigas, 
 fig. 89 (d) ; Beyrichia, Cytherina , Cyproides, fig. 
 90; Trinucleus caractaci, fig. 93 (1) ; Hemicriptu- 
 rus, fig. 97 (2) ; Illcenus barriensis fig. 98 (3) ; 
 Dalmania selenurus, fig. 118 (1) ; Phacops bufo, 
 fig. 124 (6); Dalmania calliteles, fig. 124 (7); 
 Phacops nupera, fig. 138 (2) ; Cyphaspis girarde- 
 auensis, fig. 145 (2) ; Homalonotus dekayi, figs. 
 134, 135. 
 
 Note A, p. 280, the author remarks; “ We 
 now know the following trilobites, all of which 
 belong to a slate beneath the Calciferous ; viz, 
 Atops punctatus, Eliptocephalus (I’aradoxides) 
 asaphoides, Paradoxides thompsoni, P. vermonti, 
 P. macrocephalus, Paradoxides ( Pagura ) qua- 
 drispinosus, and Microdiscus quadrico status.” 
 
 Dr. E. Emmons uses the name Pagura as a 
 subgenus to Paradoxides without indicating 
 his intention with regard to the genus. He may 
 have intended it to replace tho generic name 
 of Peltura ( Olenus ) holopyga Hall, 12th Kept. 
 New York State Cab. Nat. Hist., p. 61, which 
 in the 13th Rept. New York State Cab. Nat. 
 Hist., p. 118, is used for the typo of Bathynotus 
 
 Hall, 1860. 
 
 The preface of the manual is dated Kaleigh, 
 May 1, 1859. 
 
 Emmrich (H. F.) De Trilobitis disser- 
 tatio petrefactologica quam consensu et 
 auctoritate amplissimi philosopliorum 
 ordinis, etc. Berolini, 1839, 1 pi. 
 
 Classifies 65 species and 9 genera and 6 sub- 
 genera, as follows : 
 
 1. Phacops. 
 
 f Sec. 1. Ogygia. 
 
 2. Asaphus. 
 
 3. Ilhenus. 
 
 4. 
 
 2. Asaphus 
 
 3. Calymene 
 
 j Sec. 1. Calymene. 
 t 2. Trimerus. 
 
28 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 6; 
 
 Emmrich (H. F.) — Continued. 
 
 4. Depleura. 
 
 5. Conocephalus. 
 
 6. Ellipsocephalus. 
 
 7. Ampyx. 
 
 8. Paradoxides. 
 
 9. Odontopleura. 
 
 10. Cyphaeus. 
 
 * Zur Naturgesehichte der Trilobiten. 
 
 Programm zur offentlichen Priifung, 
 welclie mit den Zoglingen der Real- 
 echule in Meiningen Donnerstag dein 
 28. und Freitag den 29. Marz 1&44 im 
 grossen Horsaale der Anstalt abgehal- 
 ten werden soil, etc. Meiningen, 1844, 
 lpl. 
 
 Pt. 1 . Zur Morphologie der Trilobiten, pp. 4- 
 13. 
 
 Pt. 2. Ueber die Trilobiten gattungen, pp. 
 13-18. 
 
 Pt. 3. Ueber die Verbreitung der Trilobiten 
 in den Gebirgsschichten, pp. 18-28. 
 
 The genera are arranged into 25 families in 
 the following order : 
 
 1. Phacops, Dalmania n. g., 2. Phillipsia, 3. 
 Griffithides, 4. Gerastos , 5. Asaphus , 6. Illcenus, 
 7. Ogygia, 8. Bronteus, 9. Nuttama. 10. Bncri 
 nurus n. g., 11. Amphion, 12. Calymene, 13. Ho- 
 malonotus, 14. Conocephalus , 15. Ellipsocepha- 
 lus, 16. Anthes, 17. Paradoxides, 18. Odonto- 
 pleura, 19. Arges, 20. Cnyptolithus, 21. Ampyx, 
 22. Olenus , 23. Remopleurides, 24. Ceraurus, 25. 
 Agnostus. 
 
 Ueber die Trilobiten. 
 
 In Neues Jahrbuch fiir Mineral., 1845 n 18 
 lpl. 
 
 For list of genera, see preceding reference. 
 
 On the morphology, classification, 
 
 and distribution of the Trilobites. 
 
 Scientific Memoirs, edited by Richard Tay- 
 lor, vol. 4, 1846, pt. 14, p. 253, 1 pi. 
 
 Translation of the preceding reference. 
 
 E&mark (H. M. T.) Om nogle nye Arten 
 af Trilob iter. (*) 
 
 In Mag. for Naturvidensk., andre Raekke, 
 Christiania, vol. 1, 1833, p. 268, pi. 8. 
 
 Trilobiter asellus, T. elliptifrons, T. sphoerius , 
 T. semilunaris, T. dentatus. 
 
 Etheridge (Robert). Description of the 
 Palaeozoic and Mesozoic fossils of 
 Queensland. 
 
 In Quart. Jour. Geol. Soc. London, vol. 28 
 1872, p. 317. 
 
 GriJJlthides dubius, pi. 18, fig. 7. 
 
 • Memoirs Geological Survey of Scot- 
 
 land. Edinburgh, 1873. 
 
 Expl. Map 23, p. 93. 
 
 Ceratiocaris. 
 
 ■ Observations on a few Graptolites 
 
 from the Lower Silurian rocks of Vic- 
 
 J Etheridge (Robert) — Continued. 
 
 toria, Australia, with a further note o: 
 the structure of Ceratiocaris. 
 
 In Annals Mag. Nat. Hist., London, 4th s< 
 ries, vol. 14, 1874. p. 1. 
 
 On the remains of a large Crustacea] 
 probably indicative of a new species o: 
 Eurypteridw, or allied genus (Eurypteru, 
 stevensoni), from the Lower Carbonifer 
 ous series (Cementstone group) of Ber 
 wickshire. 
 
 In Qiiart. Jour. Gcol. Soc. London, vol. 33 
 
 1877, p. 223, 2 figs. 
 
 Palaeontology of the coasts of the 
 
 Arctic lands visited by the late Brit- 
 ish expedition under Capt. Sir George 
 Mares, etc. 
 
 In Quart. Jour. Geol. Soc. London, vol. 34 
 
 1878, p. 568. 
 
 Proetus , Calymene, Asaphus, Encrinurus 
 Bronteus. 
 
 On the occurrence of the genui 
 
 Dithyrocaris in the Lower Carbonifer- 
 ous or Calciferous sandstone series of 
 Scotland, and on that of a second spe- 
 cies of Anatlirapaloemon in these beds. 
 
 In Quart. Jour. Geol. Soc. London, vol. 35, 
 
 1879, p. 464, pi. 23. 
 
 Dithyrocaris, Anthrapalcemon. 
 
 On the occurrence of a small new 
 
 Phyllopod Crustacean, referable to the 
 genus Leaia in the Lower Carbonifer- 
 ous rocks of Edinburgh. 
 
 In Annals Mag. Nat. Hist., London, 5th se- 
 ries, vol. 3, 1879, p. 257. 
 
 and Nicholson (H. A. ) See Nichol- i 
 
 son (H. A.) and Etheridge (Robert). I 
 
 and Salter (J. W.) See Salter (J. 
 
 W.) and Etheridge (Robert). 
 
 Notes on a collection of fossils from I 
 
 the Palaeozoic rocks of New South 1 
 Wales. 
 
 In Proc. Royal Soc. New South Wales, vol. 
 19, 1880, p. 247, 1 pi. 
 
 Encrinurus punctatus. 
 
 Address of the President. 
 
 In Quart. Jour. Geol. Soc. London, vol. 37, 
 1881, p. 37. 
 
 Reports of the committee, consisting 
 
 of Mr. R. Etheridge, Dr. Henry Wood- jj 
 ward, and Prof. T. Rupert Jones, sec- i 
 retary, on the fossil Phyllopoda of the 
 Palaeozoic rocks. 
 
 See Reports of the secretary, recorded under 
 Jones (T. Rupert). See, also, Woodward 
 (Henry) and Etheridge (Robert) ; Huxley (T. 
 H.) and Etheridge (Robert). 
 
iGDES.J 
 
 LIST OF AUTHORS. 
 
 29 
 
 theridge, jr. (Robert). On the occur- 
 rence of a raacrurous decaped ( Anthra - 
 plcemon woodwardi sp. nov.) in the Red 
 Sandstone or lowest group of the Car- 
 boniferous formation of the southeast 
 of Scotland. 
 
 In Quart, Jour. Geol. Soc. London, vol. 33, 
 1877, p. 863, pi. 27. 
 
 — On Pinnocaris lapworthi. 
 
 Proc. Royal Phys. Soc., 1878, vol. 4, p. 167. 
 Pinnocaris n. g. 
 
 — On the genus Conocephalites. 
 
 In Proc. Royal Soc. Tasmania, June, 1882, p. 
 152. 
 
 ’eistmantel ( Ottokar ). Ueber ein neues 
 Vorkommen von nordischen silurischen 
 Diluvilgeschieben bei Lampersdorf in 
 der Grafschaft Glatz (Zeitschrift Lotos, 
 Dec., 1874, p. 10, Prag). 
 
 Phacops downingice, Leperditia marginata. 
 Fischer (G. de Waldheim). Notice sur 
 l’Eurypterus de Podolie et le Chiro- 
 therium de Livonie. Moscou, 1839, 2 
 pis. 
 
 JEurypterus remipes,E. lacustris?, E. tetra- 
 gonoijhthalmus n. s. 
 
 Pitch (Asa). Fossils of Washington 
 County, New York. 
 
 In Trans. New York Agric. Soc., vol. 9, 1850, 
 
 p. 862. 
 
 Atops trilineatus , Olenus asaphoides, Trinu- 
 cleus concentrica. 
 
 Fletcher (W. F.) Observations on Dud- 
 ley Trilobites. 
 
 In Quart. Jour. Geol. Soc. London, vol. 6, 1850, 
 p. 235, pis. 27, 27 bis. 
 
 IAchas bucklandi, L. hirsutus, L. grayii, L. 
 salteri, L. barrandii. 
 
 Observations on Dudley Trilobites. 
 
 Part 2. 
 
 In Quart. Jour. Geol. Soc. London, vol. 6, 1850, 
 p. 402. pi. 32. 
 
 Cybele punctata, C. variolaris. 
 
 Poerste (A. F.) The Clinton group of 
 Ohio. 
 
 In Bull. Denison Univ.,vol. 1, 1885, p. 65, 2 pis. 
 Acidaspis Bathyurus?, Illcenus, Calymene , 
 Lichas, Arionellus?, Dalmanites. 
 
 The Clinton group of Ohio. Pt. 2. 
 
 In Bull. Denison T7niv.,vol. 2, 1887, p. 89, pi. 8. 
 Proetus, Phacops, Dalmanites, Calymene, 
 Lichas, Illcenus, Acidaspis, Ceraurus, Encri- 
 
 nurus. 
 
 Note on Ilkeni. 
 
 In Fifteenth Rept. Geol. Nat. Hist. Survey 
 Minnesota, 1886, p. 478. 
 
 lUcenus minnesotensis, I. herricki, I. ambi- 
 gnus, I. insignis Hall. 
 
 Foerste (A. F.) — Continued. 
 
 Notes on Palaeozoic fossils. Pt. 2. 
 
 In Bull. Denison Univ., vol. 3, pt. 2, 1888, p. 
 117, pi. 13. 
 
 Phacops, Lichas, Sphcerexochus, Encrinurus , 
 Microdiscus. 
 
 Forbes (Edward). Description of Ampyx 
 nudus. 
 
 In Mem. Geol. Survey United Kingdom, de- 
 cade 2, London, 1849, pi. 2. 
 
 Ampyx nudus, Bracharnpyx n. g. 
 
 Ford (S. W.) Description of some new 
 species of Primordial fossils. 
 
 In Am. Jour. Sci., 3d series, vol. 3, 1872, p. 
 419. 
 
 Agnostus nobilis. 
 
 Descriptions of new species of fos- 
 sils from the Lower Potsdam group at 
 Troy, New York. 
 
 In Am. Jour. Sci., 3d series, vol. 6, 1873, p. 137. 
 
 Microdiscus speciosus, Leperditia troyensis. 
 
 Note on the discovery of a new local- 
 ity of Primordial fossils in Rensselaer 
 County, New York. 
 
 In Am. Jour. Sci., 3d series, vol. 9, 1875, p. 204. 
 
 Conocephalites (Atops) trilineatus Emmons. 
 
 On additional species of fossils from 
 
 the Primordial of Troy and Lansing- 
 burg, Rensselaer County, New York. 
 
 In Am. Jour. Sci., 3d series, vol. 11, 1876, p. 369. 
 
 Microdiscus meeki. 
 
 Note on Microdiscus speciosus. 
 
 In Am. Jour. Sci., 3d series, vol. 13, 1877, p. 141. 
 
 On some embryonic forms of Trilo- 
 bites. 
 
 In Am. Jour. Sci., 3d series, vol. 13, 1877, p. 
 265, pi. 4. 
 
 Metamorphoses of Olenellus ( Elliptocephalus ) 
 asaphoides. 
 
 Description of two new species of 
 
 Primordial fossils. 
 
 In Am. Jour. Sci., 3d series, vol. 15, 1878, p. 124. 
 
 Solenopleura nana. 
 
 Note on the development of Olenellus 
 
 asaphoides. 
 
 In Am. Jour. Sci., 3d series, vol. 15, 1878, p. 129. 
 
 Life of the Silurian age. 
 
 New York Tribune Extra, September 2, 1879. 
 
 In this paper Mr. S. W. Ford gives generic 
 figures of Trilobites, including figures of Mi- 
 crodiscus speciosus. 
 
 Note on the Trilobite Atops trilinea~ 
 
 tus Emmons. 
 
 In Am. Jour. Sci., 3d series, vol. 19, 1880, p. 152. 
 
 On additional embryonic forms of 
 
 Trilobites from the Primordial rocks of 
 Troy, New York, with observations on 
 
30 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA, 
 
 [bull. 63. 
 
 Ford (S. W.) — Continued, 
 the genera Olenellus , Paradoxides, and 
 Hydrocephalus. 
 
 In Am. Jour. Sci., 3d series, vol. 22, 1881, p. 250, 
 13, figs. 
 
 Note on the age of the Swedish Para- 
 doxides beds. 
 
 In Am. o our. Sci., 3d series, vol. 32, 1886, p. 473. 
 
 and Dwight (W. B.) Preliminary 
 
 report of S. W. Ford and W. B. Dwight 
 upon fossils obtained in 18*5 from meta- 
 morphic limestones of the Taconic 
 series of Emmons, at Canaan, New 
 York. PI. 7. 
 
 In Am. Jour. Sci., 3d series, vol. 31, 1886, p. 248. 
 
 Genal spine of Trilobite, perhaps Asaphus 
 megistos. 
 
 Freeh (Fritz).. Ueber das Devon der 
 Ostalpen. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 39, 1888, p. 659. 
 
 Phacops , Cheirurus, Encrinurus, Arethusina. 
 
 Die palaozoischen Bildungen von 
 
 Cabrieres, etc. 
 
 Inr Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 39, 1887, p. 360, pi. 24. 
 
 Harpes, Phacops , Proetus, Dechenella, Lichas, 
 Cheirurus, Bronteus, Ogygia. 
 
 Gehler ( J. C. ) De quibusdam varioribus 
 agri Lipsiensis petrificatis. Spec. I. 
 Trilobites f. Entomoslithus paradoxus 
 Linnd. Lipshe, 1793 [1 pi.]. 
 
 The author gives a sketch of the bibliography 
 of the Trilobites, and figures several specimens 
 of Calymene blumenbachii. 
 
 Geinitz (H. B.) Grundriss der Verstei- 
 nerungs-Kunde. Dresden, 1846, 28 pis. 
 
 Limulus. Halicyne, Belinurus, Eurypterus, 
 Cytherina, Calymene, Homalonotus, Dipleura, 
 Trimerus, Cyphaspis, Phacops, Aconia, Illcenus, 
 Archegonus, Asaphus, Dysplanus, Nileus, Am- 
 pyx, Trinucleus, Ogygia, Odontopleura, Arges, 
 Bronteus, Paradoxides, Olenus, Conocephalus, 
 Ellipsocephalus, Harpes, Cytherea, Cypridina, 
 Cyprella, Cypridella , Pollicipes, Cyclus. 
 
 Carbonformation und Dyas in Ne- 
 braska. Dresden, 1866, 5 pis. 
 
 Phillipsia sp. ?, Cythere. 
 
 Genzmar. Beschreibung einer ver- 
 steinerten Muschel mit dreifachen 
 Riicken. (*) 
 
 In Gesell. der Ober-Lausitz Lobau, vol. 2, 
 1758; also, vol. 3, p. 185, fig. 17-21 ; Heues, Mag., 
 Hamburg, 1772. 
 
 This author gives a description of the Trilo 
 bites of Mecklenburg, especially those of his 
 own collection. 
 
 Gerstacker (A.) In Bronn’s Die Klassen 
 und Ordnungen der Arthropoden wis- 
 
 Gerstacker (A.)— Continued, 
 senschaftlich dargestellt in Wort und 
 Bild. Crustacea. Leipzig und Heidel- 
 berg, 1866-79, p. 1142, pis. 43-49. 
 
 Agnostus, Homalonotus , Phacops, Dalmani- 
 tes, Cheirurus , Cromus, Deiphon, Stauroce- ' 
 phalus, Ampyx, Hydrocephalus, Acidaspis, Te- . 
 lephus, JEglina, Lichas, Sphcerexochus, Triar- 
 thrus, Dindymene, Barrandia, Illcenus, Nileus, \ 
 Ogygia. Bronteus, Asaphus, Paradoxides, Phil - 4 
 lipsia, Carmon, Ellipsocephalus, Cyphaspis, 
 Arethusina, Proetus, Arionellus , Remopjeurides, | 
 Bohemilla, Calymene, Conocephalit ^ Olenus, 
 Peltura, Arera, Sao, Phacoparia, Amphion, * 
 Encrinurus, Zethus. Trinucleus, Dionides. Har- ■. 
 pides, Harpes, Aristozoe, Beyrichia, Bolbozoe, [ 
 Callizoe, Caryon, Crescentilla Cythere, Cythe- jj 
 ropsis, Elpe, Entomis , Heppa, Leperditia, Iso- 
 chilina . Orozoe, Nothozoe, Primitia, Zonozoe, ~ 
 Cryptocaris, Aptychopsis, Adelophthalmus, Eu- 
 rypterus, Limulus, Pterygotus, Belinurus, Prest- 
 wichia, Hemiaspis. 
 
 Giebel (C.) Die silurische Fauna des 
 Unterharzes. 
 
 In Abhandl. Hat. Yereins Sachsen u. Thii- 
 ringen, vol. 1, 1858, p. 1, 7 pis. 
 
 Harpes, Proetus, Cyphaspis, Phacops, Lichas, 
 Dalmannia, Acidaspis, Bronteus. 
 
 Goldfuss (A.) Observation sur la place 
 qu’occupent les Trilobites dans le rkgne" 
 animal. 
 
 In Annales Sci. Hat. Paris, vol. 15, 1828, p. 83, 
 pi. 2. 
 
 Asaphus, Calymene. 
 
 Catalogue des Trilobites. 
 
 In B andbuch der Geognosie von de la Beche, 
 1832. 
 
 This list was copied by Dr. Jacob Green in 
 his “Monograph of the Trilobites of Horth 
 America,” p. 20. 
 
 Beitrage zur Farailie der fossilen 
 
 Crustaceen . 
 
 In Hova Acta Physico Med., vol. 19, 1839, 
 Breslau, p. 353, pi. 33. 
 
 Harpes n. g., Arges n. g., Brontes n. g., II- . 
 Icenus? triacanthus. 
 
 Systematische Uebersicht der Trilo- 
 
 biten und Beschreibuug einiger neuen 
 Arten. 
 
 In Heues Jahrbnch fiir Mineral., 1843, p. 537, 
 pis. 4-6. 
 
 Harpes, Paradoxides , Olenus, Antlics n. g., 
 Olenus scaraboeoides, Conocephalus, Ellipsoce* 
 phalus , Proetus, Acaste, Gerastos n. g., Phacops , ' 
 Calymene, Homalonotus , Dipleura, Cryptoli-% 
 thus, Ampyx, Asaphus, Isotehis, Sympliysurus * 
 II. g., Ogygia, Cryptonymus, Odontopleura , q 
 Ceraurus, Otarion, Arges, Zethus, Amphion , . 
 Bronteus , Illcenus, Bumastus, Nileus, Agnostus. 
 
 Classifies 204 species under 32 genera. 
 
V0GDE8.J 
 
 LIST OF AUTHORS, 
 
 31 
 
 Goodchild (J. G.) and Postlethwaite 
 (J.). See Postlethwaite (J. ) and 
 Goodchild (J. G.). 
 
 Green (Jacob). Synopsis of the Trilo- 
 bites of North America. In which some 
 new genera and species are proposed. 
 
 Monthly Am. Jour. Geology, Phila., vol. 2, 
 1832, p. 558, pi. 14. Republished in Dr. Jacob 
 Green’s “ Monograph of the Trilobites of North 
 America,’' Phila., 1832. List given in Dr. R. 
 Harlan’s “Med. Phys. Researches,” Phila., 
 1835, p. 300. > 
 
 Calymene blumenbachii , C. callicephala, C. 
 r selenecephala. C. platys, C. microps, C. ancldops, 
 
 C. diops, G. bufo, Asaphus caudatus, A. selenu- 
 rus, A. pleuroplyx, A. wetherilli, A. micrurus, 
 A. limulurus, A. laticostatus, Tnmerus n. g., 
 T. delphinocephalus (pi. 14, fig. 1), Cryptolithus 
 n.g., G. tessellatus (pi. 14, fig. 4), Bipleura n. g., 
 
 D. dekayi (pi. 14, figs. 8, 9), Isotelus gigas, I 
 planus, I. cyclops (pi. 14, fig. 7), Triarthrus n. 
 g., T. beckii (pi. 14, fig. 6 ),Paradoxides boltonii 
 (pi. 14, fig. 5), Ceraurusn. g., 0. pleur exanthe- 
 mas (pi. 14, fig. 10). 
 
 A monograph of the Trilobites of 
 
 North America, with colored models of 
 the species. Philadelphia, 1832, 94 pp., 
 
 1 pi. (Oct. 1, 1832). 
 
 Calymene, Asaphus, Hemicrup turus n. g., 
 Ogygia, Isotelus, Cryptolithus, Dipleura, Tri- 
 merus, Ceraurus, Triarthrus, Nuttainia, Bron- 
 
 gniartia. 
 
 A supplement to the monograph of 
 
 the Trilobites of North America, with 
 colored models of the species. Phila- 
 delphia, 1835, 24 pp. (May 1, 1835). 
 Paradoxides, Calymene, Asaphus. 
 
 A new Trilobite. Letter to the 
 
 editor, Dec. 26, 1832. 
 
 In Am. Jour. Sci., 1st series, vol. 23, 1833, p. 
 397. 
 
 Asaphus myrmecoides. 
 
 Description of a new Trilobite from 
 
 Nova Scotia. 
 
 In Trans. Geol. Soc. Pennsylvania, vol. 1, pt. 
 1, 1834, p. 37, pi. 4. 
 
 Asaphus crypturus. 
 
 Description of some new North 
 
 American Trilobites. 
 
 In Am. Jour. Sci., 1st series, vol. 25, 1834, p. 
 
 334. 
 
 Calymene odontocephalus, Asaphus astragalo- 
 tes, A.'tetragonocephalus, Paradoxides harlani' 
 
 Description of a new Trilobite. 
 
 In Am. Jour. Sci., 1st series, vol. 32, 1837, p. 
 
 167. 
 
 Calymene phtyctainodes, Asaphus platypleu • 
 
 rus. 
 
 ■ Description of two new species of 
 
 Trilobites. Read Jau. 24, 1837. 
 
 Green (Jacob)— Continued. 
 
 In Jour. Acad. Nat. Sci. Phila., vol. 7, 1837, p. 
 217, 2 wood-cuts. 
 
 Cryphceus n, g., C. boothi, Asaphus trimblii. 
 
 J. W. Salter (Mon. Brit. Tril., p. 15) gives the 
 following diagnosis of the genus, and uses it 
 as a subgenus to Phacops: “ Form of moderate 
 size, depressed. Glabella depressed, not much 
 expanded in front; all the lobes distinct, the 
 front ones not greatly enlarged, genal angles 
 long-spined. Pleura truncate, and the hinder 
 ones often produced into spines. Tail large, of 
 many segments; the margin spinose.” 
 
 Description of several new Trilo- 
 bites. 
 
 In Am. Jour. Sci., 1st series, vol. 32, 1837, p. 
 343, 2 wood-cuts. 
 
 Cryphceus, C. boothi, C. collitelus, Trimerus 
 jacksonii, Asaphus trimblii. 
 
 — — Some remarks on the genus Para- 
 doxides Brong., and the necessity of pre- 
 serving the genus Triarthrus , proposed 
 in the Monograph of the Trilobites of 
 North America. 
 
 In Am. Jour. Sci., 1st series, vol. 33, 1838, p. 
 341. 
 
 Description of a new Trilobite. 
 
 In Am. Jour. Sci., 1st series, vol. 33, 1838, p. 
 406. 
 
 Calymene rowii. 
 
 This Trilobite was figured by Mr. Row in the 
 Poughkeepsie Telegraph, Nov. 22, 1837. 
 
 Description of a new Trilobite. 
 
 In Annals Mag. Nat. History, 1st scries, vol. 
 1, 1838, p. 79. 
 
 Calymene rowii. 
 
 The inferior surface of the Trilobite 
 
 discovered. 
 
 In The Friend, a weekly Journal, Philadel- 
 phia, March 16, 1839. 
 
 Calymene bufo. 
 
 The inferior surface of the Trilobite 
 
 discovered. Illustrated, with colored 
 models. Philadelphia, 1839. 
 
 Calymene bufo. 
 
 Remarks on the Trilobites. 
 
 In Am. Jour. Sci., 1st series, vol. 37, 1839, p. 
 25. 
 
 This article appears to be a republicalion of 
 the two preceding references, with the addition 
 of the remarks on p. 38 of the Journal 
 
 An additional fact, illustrating the 
 
 inferior surface of Calymene bufo. 
 
 In Am. Jour. Sci., 1st series, vol. 38, 1810, p. 
 410. 
 
 Grewingk (C.) Geologie von Liv- and- 
 Kurland. 
 
 In Archiv Natur. Liv-, Ehst- u. Kurl., Dor- 
 pat, vol. 2, pt. 3, 1861, p. 571, 4 pis. 
 
 Beyrichia. 
 
32 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Griffith (Richard). 
 
 Two important works on the paleontology 
 and geology of Ireland were prepared under 
 the direction of Mr. Richard Griffith by Fred- 
 erick McCoy, who will be counted as the 
 author, although Mr. Richard Griffith was the 
 collector of the specimens and the financial 
 supporter of the publications. 
 
 The contributions on the Paleozoic Crustacea 
 are given under McCoy (Frederick) in this 
 work. 
 
 Grote (A. R.) and Pitt (W. H.) New 
 specimen from the Water Lime group 
 at Buffalo, N. Y. 
 
 In Proc. Am. Assoc. Adv. Sci., 26th meet- 
 ing, Nashville, 1877, p. 300. 
 
 Pterygotus cummingsi. 
 
 Description of a new Crustacean 
 
 from the Water Lime group at Buffalo. 
 
 In Bull. Buffalo Soc. Nat. Sci., vol. 3, 1875, 
 
 p. 1. 
 
 Eusarcus n. g. 
 
 On new species of Eusarcus and 
 
 Pterygotus from the Water Lime group 
 at Buffalo. 
 
 In Bull. Buffalo Soc. Nat. Sci., vol. 3, 1875, p. 
 17, plate? 
 
 Eusarcus , Pterygotus. 
 
 Gruenwaldt (M.) Beitrage zur Kennt- 
 niss der sedimentaren Gebirgsforma- 
 tionen des Ural. 
 
 In Mem. Acad. Sci. St.-P6tersbourg, 7th se- 
 ries, vol. 2, No. 7, 1860, 6 pis. 
 
 Phillipsia, Leperditia. 
 
 Guettard (E.-T.) M^moiresur les ardoi- 
 sibres d’Angers. 
 
 InM6m. Acad. Sci. Paris, 1757, p. 52, pis. 7-9. 
 Reprint: Amsterdam, 1768. 
 
 The author in his memoir on the geology of 
 Angers gives descriptions and figures of several 
 Trilobites. These were afterwards described 
 by Alex. Brongniart under the genus Ogygia 
 and named by this author Ogygie de Guettard 
 and O. desmarestii. 
 
 Haldeman ( S. S. ) On the supposed iden- 
 tity of Atops trilineaius with Triarthrus 
 becJcii. 
 
 In Am. Jour. Sci., 2d series, vol. 5, 1848, p. 
 107. 
 
 Hall (Charles E.) Contribution to palae- 
 ontogy from the Museum of the Second 
 Geological Survey of Pennsylvania. 
 
 In Proc. Am. Philos. Soc., Phila., vol. 16, 1877, 
 
 p. 621. 
 
 Eurypterus. 
 
 Hall (James). Description of two species 
 of Trilobites belonging to the genus 
 Paradoxides. 
 
 Hall (James) — Continued. 
 
 In Am. Jour. Sci., 1st series, vol. 33, 1838, p. 
 139, 2 figs. 
 
 Read before th e T ale N at ural History Society, 
 March 21, 1837. 
 
 Paradoxides beckii , P. eatoni. 
 
 Trilobites of the inferior strata. 
 
 (Extracted and published in advance of the 
 “Palaeontology of New York,” vol. 1, Albany, 
 1846, p. 225, pis. 60-67.) 
 
 Olenus, Phacops, Calymene, Platynotus, Tri- 
 nucleus, Asaphus Isotelus, Acidaspis, Ceraurus , 
 lllcenus , Agnostus. 
 
 Palaeontology of New York. Yol. 1. 
 
 Containing descriptions of the organic 
 remains of the lower divisions of the 
 New York system. Albany, 1847, LOO 
 pis. 
 
 Olenus , Phacops , Calymene, Platynotus , Tri- 
 nucleus, Asaphus , Isotelus, Acidaspis, Cerau- 
 rus, lllcenus, Agnostus. 
 
 Remarks on the observations of S. 
 
 S. Haldeman “ On the supposed iden- 
 tity of Atops trilineatus with Triarthrus 
 beckii.” 
 
 In Am. Jour. Sci., 2d series, vol. 5, 1848, p. 322, 
 10 wood-cuts. 
 
 Descriptions of new species of fos- 
 sils, and observations upon some others 
 previously not well known, from the 
 Trenton limestones. 
 
 In Third Rept. New York State Cab. Nat. 
 Hist., 1850, p. 167, 5 pis. (2 eds.). 
 
 Asaphus extans. 
 
 This species was used by Mr. E. Billings for 
 the type of Bathyurus. 
 
 Description of new or rare species of 
 
 fossils from the Palaeozoic series. 
 
 In Rept. Geol. Lake Superior Land Dist. 
 (Foster and Whitney), 1851, pt. 2, p. 203, pis. 
 22-35. 
 
 Harpes escanabice, Dikelocephalus , Proetus, 
 Phacops anchiops, P. callicephalus, Asaphus 
 barrandi-, tracks of a Crustacean ? 
 
 Palaeontology of New York. Yol. 2. 
 
 Containing descriptions of the organic 
 remains of the lower divisions of the 
 New York system. Albany, 1852, 104 
 pis. 
 
 Phacops, Proetus, Calymene, Homalonotus, 
 Arges, Lichas, Acidaspis, Ceraurus, Cybele, 
 Bumastis, Beyrichia, Cytherina, Onchus. 
 
 Noies on some fossils of the so-called 
 
 Taconic system described by Doctor 
 Emmons. 
 
 In Am. Jour. Sci., 2d series, vol. 19, 1855, p. 
 434. 
 
 Olenus ( Ell^ptocephalus ) asaphoides. 
 
VOGDES.] 
 
 LIST OF AUTHORS, 
 
 33 
 
 Hall (James) — Continued. 
 
 Description of new species of fossils 
 
 from the Carboniferous limestone of In- 
 diana and Illinois. 
 
 Read in 1856 and published separately by the 
 author. See, also, Trans. Albany Inst., vol. I, 
 pt. 1, 1857, p. 1. 
 
 Cytherina carbonaria. 
 
 Descriptions of these fossils, with additional 
 notes by R. P. Whitfield, were published in the 
 Bull. Am. Mus. Nat. Hist., New York, vol. 1, No. 
 3, 1882. 
 
 The original descriptions, with additional ob- 
 servation by James Hall, with the plates from 
 R. P. Whitfield’s memoir, were published in the 
 12th Annual Rept. Geol. Nat. Hist. Indiana, 
 1882, pp. 321-375, pis. 29-32. 
 
 The Trilobites of the shales of the 
 
 Hudson River group. 
 
 In Twelfth Rept. New York State Cab. Nat. 
 Hist., 1859, p. 59, 3 wood-cuts. See, also, Pa- 
 laeont. New York, vol. 3, 1859; Geol. Vermont, 
 vol. 1, 1861 ; 13th Rept. New York State Cab. 
 Nat. Hist., 1860. 
 
 Olenus thornp8oni, O. vermontana, Peltura 
 ( Olenus ) holopyge. 
 
 Geological Survey New York. Palae- 
 ontology. Yol. 3. Containing descrip- 
 
 ' tions and figures of the organic remains 
 of the Lower Helderberg group and the 
 Oriskany sandstone. 1855-’59. 
 
 Pt. 1, text, 1859; pt. 2, plates, 1861, 120 pis. 
 
 Proetus, Phacops, Dalmania, Homalonotus, 
 Licha8, Acidaspis , Bronteus, Eurypterus, Doli- 
 chopterus n. subgenus, Pterygotus, Leperditia , 
 Beyrichia, Ceratiocaris, Olenus thompsoni, O. 
 vermontana, Peltura {Olenus) holopyge. 
 
 Description of new species of fossils 
 
 from the Silurian rocks of Nova Scotia. 
 
 In Canadian Naturalist, vol. 5, 1860, p. 144. 
 
 Homalonotus dawsoni Hall, Calymene blu- 
 menbachii , Dalmania logani Hall, Beyrichia 
 pustulosa Hall, B. ceqilatera Hall, Leperditia 
 sinuata Hall. 
 
 Contributions to palaeontology, 1858 
 
 and 1859. Notes and observations upon 
 the fossils of the Goniatite limestone in 
 the Marcellus shale of the Hamilton 
 group in the eastern and central parts 
 of the State of New York, and those of 
 the Goniatite beds of Rockford, In- 
 diana ; with some analogous forms from 
 the Hamilton group proper. 
 
 In Thirteenth Rept. New York State Cab. 
 Nat. Hist., 1S60, p. 95. 
 
 Proetus doris Hall. 
 
 Note upon the Trilobites of the shales 
 
 of the Quebec group in the town of 
 Georgia, Vermont. 
 
 Bull. 63 3 
 
 Hall (James) — Continued. 
 
 In Thirteenth Rept. New York State Cab. 
 Nat. Hist., I860, p. 113. 
 
 Barrandia n. g. 
 
 This term was used by Frederick McCoy, 
 in 1844, for a genus of Trilobites. 
 
 Bathynotus n. g. 
 
 New species of fossils from the Hud- 
 son River group of Ohio and the West- 
 ern States. 
 
 In Thirteenth Rept. New York State Cab. 
 Nat. Hist., 1860, p. 119. 
 
 Oalymene christyi, Proetus parviusculus. 
 
 Geological Survey of Wisconsin. 
 
 Description of new species of fossils 
 from the investigations of the survey, 
 etc. Report of the superintendent of 
 the Geological Survey, exhibiting the 
 progress of the work, January 1, 1861, 
 
 p. 11. 
 
 Dalmanites , Oalymene, lllcenus. 
 
 Preliminary notice of the Trilobites 
 
 and other Crustacea of the Upper 
 Helderberg, Hamilton, and Chemung 
 groups. 
 
 Author’s edition, published in 1861, 11 pis., 
 170 pp. ; 15th Rept. New York State Cab. Nat. 
 Hist., 1862, p. 82. 
 
 Olenellus n. g., Proetus, Phacops, Dalmania , 
 Calymene, Homalonotus, Lichas, Acidaspis , 
 Beyrichia, Leperditia. 
 
 Note on the genus Cypricardites. 
 
 In Fifteenth Rept. New York State Cab. Nat. 
 Hist., 1861, p. 192. Plate illustrating certain 
 genera and species described by T. A. Conrad 
 in the 5th Annual Rept. Pal. Dept. New York 
 Geol. Survey, 1841, pi. 11 (reprint). 
 
 Dicranurus, pi. 11, fig. 1; Aspidolites, pi. 11, 
 fig. 2 ; Acidaspis tuberculatus, pi. 11, fig. 3. 
 
 Note upon the Trilobites of the Hud- 
 son River group, in the town of Georgia, 
 Vermont. 
 
 In Geol. Vermont, vol. 1, 1861, p. 367, pi. 13. 
 
 Barrandia, B. vermontana, Bathynotus, B. 
 holopyga. 
 
 Palaeontology of Wisconsin. Re- 
 marks upon the condition of the fossils 
 in the rocks of the several formations. 
 Catalogue of fossils known in the Palae- 
 ozoic formations of Wisconsin, with 
 observations upon some of the known 
 species and descriptions of several new 
 forms. 
 
 Geol. Survey Wisconsin, vol. 1, 1862, p. 425. 
 
 On a new Crustacean from the Pots- 
 dam sandstone. A letter addressed to 
 Principal Dawson, dated Albany, Oct. 
 31, 1862. 
 
34 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 I BULL. 63. 
 
 Hall (James) — Continued. 
 
 In Canadian Naturalist, vol. 7, 1862, p. 443, 
 figure. See The Geologist, vol. 6, London, 1863, 
 p. 247, figure. 
 
 Aglaspis n. g. 
 
 On the occurrence of Crustacean re- 
 mains of the genera Ceratiocaris and 
 Dithyrocaris , with a notice of some new 
 species from the Hamilton group and 
 Genesee slate. 
 
 In Sixteenth Kept. New York State Cab. Nat. 
 Hist., Albany, 1863, p. 71, plate. 
 
 Preliminary notice of the fauna of 
 
 the Potsdam sandstone, with remarks 
 upon the previously known species of 
 fossils, aud description of some new 
 ones from the sandstones of the Upper 
 Mississippi Valley. 
 
 In Sixteenth Kept. New York State Cab. Nat. 
 Hist., 1863, p. 119, 6 pis. Supplementary note, 
 
 p. 110. 
 
 Dikelocephalus, Triarthrella n. g., Conocepha- 
 lus , Arionellus, Chariocephalus n. g., Ptychas- 
 pis n. g., Lichas, lllcenurus n. g., AmpMon?, 
 Agntfstus, Pemphigaspis n. g., Aglaspis. 
 
 Notice of some new species of fossils 
 
 from a locality of the Niagara group in 
 Indiana, with a list of identified spe- 
 cies from the same place. 
 
 In Trans. Albany Inst., vol. 4, 1864, p. 195. 
 Author’s edition published May 2, 1863, pp. 1-34. 
 
 Dalmania, Cyphaspis, Lichas. 
 
 Plates of the species. 28th Kept. New York 
 State Mus. Nat Hist., 1879. 
 
 Account of some new or little known 
 
 species of fossils from rocks of the age 
 of the Niagara group. 
 
 In T wen t ietb Kept. N ew Y ork State C ab. N at. 
 Hist., 1867, p. 305, 21 pis. Originally printed 
 in advance for the 18th Keport New York State 
 Cab. Nat. Hist., 1864. Kevised edition, Albany, 
 1870, with 22 pis. 
 
 Dalmania , Calymene, Lichas , Acidaspis, 
 Ceraurus , Sphcerexochus, lllcenus, Encrinurus, 
 Bronteus. 
 
 Geological Survey of the State of 
 
 Wisconsin, ISfiiMfiS. Palaeontology. 
 Pt. 3. Organic remains of the Niagara 
 group and the associated limestones. 
 94 pp., 18 pis. Albany, 1871. 
 
 The same was published in 1864 in advance 
 for tbe 18th Rept. New York State Cab. Nat. 
 Hist., 1867, under tbe title of “Account of some 
 new or little known species of fossils from rocks 
 of the ago of the Niagara group.” See 20th 
 Kept. New York State Cab. Nat. Hist., rev. 
 edition, 1870, p. 347. 
 
 Hall (James) — Continued. 
 
 Descriptions of new species of fossils 
 
 from the Hudson River group in the 
 vicinity of Cincinnati, Ohio. 
 
 In Twenty-fourth Rept. New York State ' 
 Mus. Nat. Hist., Albany, 1872, p. 225, 1 pi. 
 
 Published Oct., 1871, in advance of the State , 
 Cab. report. 
 
 Leperditia, Beyrichia. 
 
 Descriptions of new species of Cri- 
 
 noids and other fossils from strata of 
 the age of the Hudson River group and 
 Trenton limestone. 
 
 In Twenty -fourth Rept. New York State 
 Mus. Nat. Hist., 1872, p. 205, 3 pis. 
 
 Dalmania breviceps, Proetus parviusculus. 
 
 Advance sheets of this article were printed i 
 and distributed in November, 1866, except the 
 first four species of Crinoidea mentioned in the 
 foot-note on p. 205, which were first published 
 in 1871 in a pamphlet entitled “ New species of 
 fossils from the Hudson River group in the I 
 vicinity of Cincinnati, Ohio.” 
 
 The fauna of the Niagara group in 
 
 central Indiana. 
 
 Documents only of Twenty-eighth Rept. 
 New York State Mus. Nat. Hist., 1876, 34 pis. "! 
 
 The fauna of the Niagara in central 
 
 Indiana. 
 
 In Twenty-eighth Rept. New York State 
 Mus. Nat. Hist., 1879, p. 99, 34 pis. 
 
 Cyphaspis , Dalmanites, Odontocephalus, Caly-~- 
 mene, Homalonotus, Lichas , Ceraurus, lllcenus , 1 
 Beyrichia , Leperditia. 
 
 Illustrations of Devonian fossils : 
 
 Gasteropoda, Pteropoda, Cephalopoda, 
 Crustacea, and Corals of the Upper 
 Helderberg, Hamilton, and Chemung 
 groups, etc. Albany, 1876, 7 pp. , 133 pis. 
 
 Proetus , Phillipsia (Brachymetopus ?), Pha- 
 cops, Dalmanites, Calymene, Homalonotus, Li - ] 
 chas, Acidaspis ( Terataspis ), Dithyrocaris , Cera- I 
 tiocaris. 
 
 Descriptions of new species of fossils | 
 
 from the Niagara formation at Waldron, 
 Indiana. 
 
 In Trans. Albany Inst., vol. 10, 1883, p. 57. I 
 Read 1879, and published separately in 1881. * 
 
 Acidaspis fimbriata , lllcenus ( Bumastus ), 1 
 Ioxus. 
 
 Description of the species of fossils (1 
 
 found in the Niagara group at Waldron, 
 Indiana. 
 
 In Eleventh Ann. Rept. for 1881, Dept. Geol. | 
 Nat. Hist. Survey Indiana, 1882, p. 217, 36 pis. I 
 
 Cyphaspis, Dalmanites, Odontocephalus. Caly • N 
 mene, Homalonotus, Lichas, Acidaspis, lllcenus , k 
 I Beyrichia, Leperditia. 
 
VOGDES.] 
 
 LIST OF AUTHORS. 
 
 Hall (James) — Continued. 
 
 Note on the Eurypteridce of the De- 
 vonian and Carboniferous formations 
 of Pennsylvania, with a supplementary 
 note on the Stylonurus excelsior. 
 
 In Proc. Ain. Assoc. Adv. Sci., 33d meeting, 
 Phila., 1884, p. 420. 
 
 Eurypteridce from the Devonian and 
 
 Carboniferous formations of Pennsyl- 
 vania. With 6 pis. 
 
 Extracted Kept. Prog. PPP., 2d Geol. Survey 
 Pennsylvania, 1884. 
 
 Note on the Eurypteridce of the De- 
 vonian and Carboniferous formations 
 of Pennsylvania. 
 
 In Second Geol. Survey Pennsylvania, Eept. 
 Prog. PPP., 1884, 6 pis. 
 
 Eurypterus, Dolichopterus, Pterygotus, Stylo- 
 nurus, Eurypterus (Anthraconectes) mazonensis 
 
 M. & W. 
 
 Description of a new species of 
 
 Stylonurus from the Catskill group. 
 
 In Thirty-sixth Eept. New York State Mus. 
 Nat. Hist., 1884, p. 76, pi. 5. 
 
 Stylonurus excelsior Hall. 
 
 There was a short notice of this species pub- 
 lished by D. S. Martin (Trans. New York 
 Acad. Sci., vol. 2, 1882, p. 8). This notice was 
 based upon a cast of the carapace in the New 
 York State Museum, which had been labeled 
 with name and locality by Prof. James Hall. 
 
 and Whitfield (R. P.) Descriptions 
 
 of new species of fossils from the vi- 
 cinity of Louisville, Ky., and the Falls 
 of the Ohio. 
 
 In Twenty-fourth Eept. New York State 
 Mus. Nat. Hist., 1872, p. 181, pi. 13, figs 20 and 21. 
 
 Illcenus cornigerus H. & W. 
 
 Geological Survey of Ohio. 
 
 Vol. 2. Geology and palamntology. 
 Pt. 2. Palaeontology. 1875, p. 67, pis. 
 
 1 - 12 . 
 
 Proetus, Dalmania , Galymene, Lichas, Encri- 
 nurus, Leperditia ( Isochilina ), Beyrichia, Plu- 
 mulites. 
 
 Palaeontology. 
 
 In U. S. Geol. Expl. 40th Parallel, vol. 4, pt. 
 2, 1877, 7 pis. 
 
 Dikellocephalus, Conocephalites, Crepicepha- 
 lus ( LoganeUus ), Ptychaspis , Ghariocephalus, 
 Bathyurus, Proetus, Ogygia, Agnostus. 
 
 • and Clarke (John M.) Geological 
 
 • Survey of the State of New York. 
 Palaeontology. Vol. VII. Text and. 
 plates, containing descriptions of the 
 Trilobites and other Crustacea of the 
 Oriskany, Upper Helderberg, Hamil- 
 ton, Portage, Chemung, and Catskill 
 groups. Albany, 1888, 236 pp., 36 pis. 
 
 35 
 
 Hall (James) and Clarke (John M.) — 
 Continued. 
 
 Trilobita : Galymene , Homalonotus, Bron- 
 teus, Phacops, Dalmanites subgen., Haus- 
 manni n. s. g., Coronura n. s. g., Cryphceus. 
 Odontocephalus, Gorycephalus, Ghasmops, Li- 
 chas subgen., Terataspis, Gonolichas . Hoplo- 
 chas , Arges , Geratolichas, Proetus , Phcethonides, 
 Gyphaspis. 
 
 Xiphosura: Protolemulus, Eurypterus , Stylo- 
 nurus. 
 
 Phyllocoridfe : Ceratiocaris, Echinocaris, Ely- 
 mocaris, Tropidocaris. 
 
 Pinsecaridae : Mesothyra n. g. 
 
 Ehinocardse: Bhinocaris n. g. 
 
 Discinocaridse : Spathiocaris, Dipterocaris. 
 
 Decapoda : Palceopalcemon. 
 
 Phyllopoda : Estheria, Schizodiscus n. g. 
 
 Cirripidae : Protobalanus. 
 
 Palseocreusia : Stropbilepis n. g., Turrilepas. 
 
 Hancock ( Abbany). Remarks on certain 
 vermiform fossils found in the mountain 
 limestone districts of the north of Eng- 
 land. 
 
 In Eept. 28th Meeting Brit. Assoc. Adv. Sci., 
 1858, Tran, of Sec., p. 80. 
 
 Tracks of Trilobites. 
 
 Harlan (Richard). Critical notices of 
 various organic remains hitherto dis- 
 covered in North America. 
 
 In Trans. Geol. Soc. Pennsylvania, vol. 1, pt. 
 
 1. 1834, p. 46, 1 pi. 
 
 The author herein describes two species of 
 Eurypterus and gives a list of North American 
 Trilobites. 
 
 Eurypterus remipes lie Kay, E. lacustris 
 Harlan. 
 
 Notice of nondescript Trilobites from 
 
 the State of New York, with observa- 
 tions on the genus Triarthrus, etc. 
 
 In Trans. Geol. Soc. Pennsylvania, vol 1, pt. 
 
 2. 1835, p. 263, pi. 15. 
 
 Paradoxides triarthrus Har., P. arcuatus 
 Har.,P. scaraboides Brong. 
 
 Medical and physical researches, or 
 
 original memoirs in medicine, surgery, 
 physiology, geology, zoology, etc. 
 Phila., 1835, 36 pis. 
 
 Contains a republication of the above articles 
 under Harlan, pp. 253-313 and 400-403. 
 
 Hartt (C. F.) Fossils of the Primordial 
 or Acadian group at St. John. 
 
 In Acadian Geology, the geological struct- 
 ure, organic remains, and mineral resources of 
 Nova Scotia, etc., by J. W. Dawson, 2d ed., 
 London, 1868, pp. 641-657; also 3d ed., 1 878, 
 with supplement (wood-cuts). 
 
 Paradoxides, Gonocepliahtes, Microdiscus, Ag- 
 nostus. 
 
 Mr. ('. F. nartt, in his original description of 
 Microdiscus dawsoni Hartt, described the spe- 
 cies under the new generic name of Dawsonia. 
 
36 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. {bull. 63. 
 
 Hartt (C. F.) — Continued. 
 
 In the Acadian Geology the species is placed 
 under the genus Microdiscus on the authority 
 of Mr. E. Billings, of the Canadian Geological 
 Survey. 
 
 Appendix B. List of New Bruns- 
 wick fossils. 
 
 See Bailey’s “Observations on the Geol. of 
 Southern New Brunswick, etc.,” 1865, p. 143. j 
 
 and Rathbun (Rickard). Morgan 
 
 Expedition, 1870- 71. On the Devonian 
 Trilobites and Mollnsks of Erer6, Prov- j 
 ince of Pard., Brazil. 
 
 In AnDals Lyceum Nat. Hist., New York, 
 vol. 11, 1875, p. 110. 
 
 Dalmania paituna H. & R., Homalonotus 
 oiara H. & R. 
 
 Herrick (C. L.)— Continued. 
 
 Appendix 2. A Waverly Trilobite. 
 
 In Bull. Denison Univ., vol. 2, pt. 1, 1887, p. 69, 
 pi. 7, fig. 14. 
 
 Phillipsia shumardi Herrick. 
 
 The geology of Licking County, 
 
 Ohio. Pt. IY. The Subcarboniferous 
 and Waverly groups. 
 
 In Bull. Denison Univ., vol. 3, 1888, p. 13, pis. 
 2, 11, and 12. 
 
 Phillipsia meramecensis Sh., P. shumardi 
 Her., P. precursor Her. 
 
 On the Trilobites of the Ohio Wa- 
 verly group. 
 
 In Author’s advance sheets from the Bull. 
 Denison Univ., vol. 4, 1889, 1 pi. 
 
 Proetus, Phcethonides, Phillipsia, Cythere. 
 
 Hauer (F. von). Ueber Barrande’s Ver- I 
 such einer Classifikation der Trilobiten. 
 
 In Sitzungsber. d. Wien. Akad. Math.-na- 
 turw, Classe, Y, p. 304, 1850. 
 
 Haulp (K.) Die Fauna der Graptkoli- 
 tengest. 
 
 In Lausitzische Mag., vol. 44, Gorlitz, 1878, p. 
 75, pi. 5. 
 
 Beynchia. 
 
 Hawle (Ignaz). See Corda (A. J. C.) 
 and Hawle (Ignaz). 
 
 Hayden (F. V.) See Meek (F. B.) and 
 Hayden (F. V.). 
 
 Heidenkain (F.) Ueber Graptholiten- | 
 fiikrende Diluvial-Geschiebe der nord- j 
 deutschen Ebene. 
 
 In Zeitschr. Deutsch. geol. GeselL, vol. 21, 
 1869, p. 143, plate. 
 
 Calymene blumenbachi, Dalmanites caudata, 
 Odontopleura ovata, O. nutica, Cyphaspis, 
 Homalonotus, Beyrichiakloeden, B. maccoyana, 
 B. tuber culatus. 
 
 Heilman (A.) Die Petrefacten Thiirin- 
 gens. Cassel, 1866, 5 pts., 24 pis. 
 
 Dalmania tuberculata, Acidaspis buchi, Para- 
 doxides spinosus. 
 
 Hermann (L. D.) Maslographia Brig®, 
 Massel, 1711, pi. 9, fig. 50; pi. 11, fig. j 
 44; pi. 12, fig. 31. 
 
 The author herein compares a fragment of 
 the pygidium of an Encrinurus to a scollop 
 shell. 
 
 Herrick (C. L.) A sketch of the geolog- 
 ical history of Licking County, accom- 
 panying an illustrated catalogue of 
 Carboniferous fossils from Flint Ridge, 
 Ohio. 
 
 In Bull. Denison Univ., vol. 2, pt. 1, 1887, p. 
 
 5, 7 pis. 
 
 Proetus, Phillipsia, GriJ/ithides, Brachyme- 
 topus, Dalmanites ?. 
 
 Notes upon the Waverly group in 
 
 Ohio. 
 
 In Am. Geologist, vol. 3, 1889, p. 94, 4 pis. (not 
 descriptive). 
 
 Hibbert (Dr.) On the fresh-water lime- 
 stone of Burdiehouse, in the neighbor- 
 hood of Edinburgh, belonging to the 
 Carboniferous group of rocks; with sup- 
 plementary notes on other fresh-water 
 limestones. 
 
 In Trans. Royal Soc. Edinburgh, vol. 13, 1836, 
 p. 169, pi. 9. 
 
 The author gives reduced figures of Euryp - 
 terus remipes De Kay and E. lacustris Harlan, 
 taken from Dr. Richard Harlan’s article on 
 “Organic Remains of North America.” 
 
 Hicks ( Henry ). Note on the genus 
 Anopolenus. 
 
 In Quart. Jour. Geol. Soc. London, vol. 21, 
 1865, p. 477, figures. 
 
 Anopolenus. 
 
 Description of new species of fos- 
 sils from the Longmynd rocks of St. 
 David’s. 
 
 In Quart. Jour. Geol. Soc. London, vol. 27, 
 
 1871, p. 399, pi. 15. 
 
 Paradoxides, Plutonia, Conocoryphe, Micro- 
 discus, Agnostus, Leper ditia?. 
 
 On some undescribed fossils from the 
 
 Menevian group, with a note on the En- 
 tomostraca by Prof. T. Rupert Jones. 
 
 In Quart. Jour. Geol. Soc. London, vol. 28, 
 
 1872, p. 173, pis. 5-7. 
 
 Anoplenus, Cerausia n g., Erinnys , Cono- 
 coryphe , Arionellus , Holocephalina, Agnostus, 
 Leperditia, Entomis. 
 
 On the Tremadoc rocks in the neigh- 
 borhood of St. David’s, South Wales, 
 and their fossil contents. 
 
 In Quart. Jour. Geol. Soc. London, vol. 29, 
 
 1873, p. 39, 3 pis. 
 
 Neseurctus n. g., Niobe. 
 
VOGDES.J 
 
 LIST OF AUTHORS. 
 
 37 
 
 Hicks (Henry) — Continued. 
 
 Descriptions of new species of fos- 
 sils from the Arenig group of St. 
 David’s. 
 
 In Quart. Jour. Geol. Soc. London, vol. 31, 
 
 1875, p. 182, 3 pis. 
 
 Phacops, Galymene, Trinucleus, Ampyx, Bar- 
 randia, JEglina, Placoparia, Illcenus , 1 llcenop- 
 sis?. 
 
 Appendix to Fossiliferous Cambrian 
 
 shales, near Caernarvon, by J. E. Marr. 
 
 In Quart. Jour. Geol. Soc. London, vol. 32, 
 
 1876, p. 135. 
 
 Caryocaris, JEglina . 
 
 Hisinger (W.) Anteckningar i physik 
 och geognosi under resor uti Sverige 
 och Norrige. Stockholm, 8 pts., 1828- 
 ’40. 
 
 The first three parts contain scarcely any- 
 thing on Crustacea; the remaining parts con- 
 tain only enumerations of fossils, without de- 
 scriptions. 
 
 Cytherina phaseolus His., pt. 5, pi. 8, fig. 3. 
 
 * Tableau des purifications de la 
 
 Suede distributes en ordre systtma- 
 tique. Stockholm, 1829. 
 
 This work enumerates 40 species of Silurian 
 Crustacea previously described by J. W. Dal- 
 man. 
 
 The second edition of this work bears the 
 title “Esquisse d’un tableau des petrifications 
 de la SuMe,” Stockholm, 1831. 
 
 This work contains 43 pages and a syste- 
 matic table of the fossils, in which 46 species 
 of fossil Crustacea are mentioned. 
 
 Lethaea Svecica, seu petrificata Sve- 
 ciae iconibus et characteribus illustrata 
 duobus supplements. Holmiae, 1837- 
 ’41, 4to, 42 pis. 
 
 The first part of this work was published in 
 1835 under the title “leones petrifica'orum 
 Sveciae. Fas. I. Aniraalia articulata et mollusca 
 Cephalopoda.” The plates, 1 to 10, were sent 
 by the author only to his friends. In 1837, 
 Lethaea Svecica was published; it contained 
 124 pages and 39 plates. The first three are 
 marked A, B, C. The fossil Crustacea de- 
 scribed in this work are those of J. W. Dal- 
 man’s Palieaderna, with copies of his descrip- 
 tions and figures. The second supplement, 
 pxtblished at Stockholm in 1840, contains eleven 
 pages and three plates. Figures and descrip- 
 tions of Galymene clavifrons, Asaphus ( Tri- 
 nucleus ) secticorni8, A. cyllarus (Trinucleus) 
 and Galymene (Gheirurus) speciosa. “Lethaea 
 Svecica, seu petriiicata Sveciae, supplementa 
 secundi continuatio,’’ was published at Stock- 
 holm in 1841; it contains six pages and three 
 plates (60-62). Figures and description of a 
 Galymene. 
 
 Hoeninghaus ( F. W. ) Besckreibung 
 iiber Abbildungen von Calymene aracli - 
 noides. Crefeld, 1835, 1 pi. '(*) 
 
 Ueber die Yersteinerungen des 
 
 Uebergangs-Tkonsckiefers von Weis- 
 senback im Dillenburgscken. (*) 
 
 In Isis (oder Encycl. Zeitung), Oken, 1830, p. 
 96 ; Nones Jahrbuch fur Mineral., 1831, p. 341. 
 
 Galymene macrophthalma. 
 
 Trilobiten der geognostiseken 
 
 Sammlung. Crefeld, 1843, plate. * (*) 
 
 Asaphus dalmani. 
 
 Harpes reflexus. Crefeld, 1847, 1 p., 
 
 lpl. 
 
 Hoffman (E.) Sammtlicke bis jetzt be- 
 kannte Trilobiten Russlands. 
 
 In Verhandl. russ. k. mineral. Gesell. zu St. 
 Petersburg, 1857-’58, p. 21, 7 pis. 
 
 Proetus, Phillipsia, Phacops , Ghasmops , 
 Galymene , Lichas, Ampyx , Asaphus , Gheirurus , 
 Sphcerexockus, Zetlius , Encrinurus, Amphion , 
 Bronteus, Illcenus , Nileus, Agnostus. 
 
 Holl (F.) Handbuch der Petrefacten- 
 kunde, etc. Dresden, 1841, p. 155. 
 
 Galymene , Asaphus, Nileus, Illcenus, Lichas , 
 Ampyx, Ogygia, Olenus, Batlus. 
 
 The author gives short descriptions of the 
 Trilobites described by Alex. Brongniart, J. 
 W. Dalman, E. Eichwald, von Schlotheim, 
 and others. 
 
 Holl (H. B.) See Jones (T. Rupert) and 
 Holl (H. B.). 
 
 Hollier (E.) On a specimen of Homalo- 
 notus delphinocephalus found at Dudley. 
 
 Trans. Manchester Geol. Soc., vol. S, 1869, 
 
 p. 28. 
 
 Holm ( Gerkard ) . Anteckningar om 
 Waklenberg’s Illcenus crassicauda. 
 
 In Svenska Vetensk. Akad. Forhandl., 1880, 
 No. 4, p. 3, Stockholm, pi. 5. 
 
 Bemerk ungen iiber Illcenus crassi- 
 cauda Wakl. 
 
 In Zeitschr. deutscli. geol. Gesell., vol. 32, pt. 
 2-4, 1880, p. 559, pi. 23. 
 
 Ueber einige Trilobiten aus dem 
 
 Pkyllograptus-Sckiefer Dalekarliens. 
 
 In Kongl. Svenska Vet. Akad. Handl.,vol. 6, 
 No. 9, 1882, pi. 5. 
 
 Pliomera tornquisti, Megalaspis dalecarlicus, 
 Ampyx pater, Agnostus tornquisti, Trilobites 
 brevifrons. 
 
 De Svenska arterna af Trilobitolag 
 
 tet Illcenus Dalman. 
 
 In Kongl. Svenska Vet. Akad. nandl., vol. 7, 
 No. 3, 1882, 6 pis. 
 
38 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BUL£. 63. 
 
 Holm (Gerhard)— Continued. 
 
 Om thoraxledernas antal lios Para- 
 
 doxides tessini Brongn. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 9, 1887, p. 408. 
 
 Om forekomsten af en Cruziana i 
 
 ofversta Olenidskiffern vid Knifvinge i 
 Vreta Kloster Socken i Ostergotland. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 9, 1887, p. 412. 
 
 Om Olenellus kjerulfi Linrs. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 9, 1887, p. 493, pis. 14, 15. 
 
 Honeyman (D.) On new localities of 
 fossiliferous Silurian rocks in e’astern 
 Nova Scotia. 
 
 In Canadian Naturalist, vol. 5, 1860, p. 293. 
 
 Dr. J. W. Dawson adds a note to this paper, 
 describing Homalonotus dawsoni Hall, fig. 1, 
 with notes on other fossils. 
 
 On the geology of Arisaig, Nova 
 
 Scotia, with a note by Prof. T. Rupert 
 Jones. 
 
 In Quart. Jour. Geol. Soc. London, vol. 26, 
 1870, P.4‘90. 
 
 The note by Prof. T. E. Jones, on p. 492, on 
 some Entomostraca from Arisaig, mentions the 
 following genera : 
 
 Beyrichia, Leperditia, Primitia. 
 
 Notes of examination by Prof. James 
 
 Hall of the Silurian collection of the 
 Provincial Museum, by the Rev. D. 
 Honeyman. 
 
 In Proc. and Trans. Nova Scotian Inst. Nat. 
 Sci., vol. 7, pt. 1, 1886, p. 14. 
 
 Asaphus ditmarsice Honeyman. 
 
 The Giant Trilobite of Moose River 
 
 Iron Mine, Nova Scotia. 
 
 In Proc. and Trans. Nova Scotian Inst. Nat. 
 Sci., vol. 7, pt. 1, 1888, p. 63. 
 
 In this article Dr. D. Honeyman refers Asa- 
 phus ditmarsice to Dr. Jacob Green’s Asaphus? 
 crypturus, giving a copy of the original descrip- 
 tion of that species from Trans. Geol. Soc. 
 Pennsylvania, vol. 1, pt. 1, 1834, p. 37. 
 
 How (Henry). Notice of the occurrence 
 of a Trilobite in the Lower Carbonifer- 
 ous limestone of Hants County. 
 
 In Proc. and Trans. Nova Scotian Inst. Nat. | 
 Sci., vol. 1, 1867, pt, 1, p. 87. 
 
 Hutton (F. W.) On a Trilobite from New j 
 Reefton, New Zealand new to Australia, j 
 
 In Proc. Linn. Soc. New South Wales, sec- 
 tion 2, vol. 2, 1887-’88, p. 257. 
 
 .Huxley (T. H.) Observations ou the 
 structure and affinities of Himanlopte- 
 ru8. 
 
 In Quart. Jour. Geol. Soc. London, vol. 12, j 
 1856, p. 34. 
 
 Huxley (T. H) and Salter (J. W.) Mono- 
 graph of the fossil Crustacea forming 
 the genus Pterygotus, with its anatomy 
 and affinities. 
 
 In Mem. Geol. Survey United Kingdom. De- 
 scription of Brit, organic remains. Monograph 
 No. 1. London, 1859, atlas of 16 pis. 
 
 and Etheridge (Robert). A cata- 
 logue of the collection of fossils in the 
 Museum of Practical Geology, with an 
 explanatory introduction. London, 
 1865. 
 
 A catalogue of the Cambrian and 
 
 Silurian fossils in the Museum of Prac- 
 tical Geology. London, 1878. 
 
 This catalogue was drawn up by Mr. E. T. 
 Newton, under Prof. T. H. Huxley’s superin- 
 tendence. 
 
 The specimens were named by Mr. Kobert 
 Etheridge, palaeontologist to the Geological 
 Survey of Great Britain. 
 
 Jackson (Charles T.) Nouveau gisement 
 de Trilobites ddcouvert pres de Boston. 
 
 In Comptes Eendus Acad. Sci. Paris, vol. 43, 
 1856, p. 883. 
 
 Paradoxides tessini, P. harlani , P. spinu- 
 losus. 
 
 Sur un moule du Paradoxides harlani. 
 
 In Comptes Eendus Acad. Sci. Paris, vol. 46, 
 1858, p. 254. 
 
 James (J. F.)”^ Catalogue of fossils of 
 Cincinnati group, published by order 
 of the Committee on Palaeontology. 
 Cincinnati, 1871. 
 
 James (U. P.) Paleontology. Cata- 
 logue of Lower Silurian fossils of Cin- 
 cinnati group, found at Cincinnati and 
 vicinity, etc. Cincinuati, April, 1875. 
 
 Supplement to Catalogue of Lower 
 
 Silurian fossils of the Cincinnati group, 
 etc. Cincinnati, July 10, 1879. 
 
 Descriptions of new species of fossils 
 
 from the Cincinnati group, Ohio and 
 Kentucky. 
 
 Iu The Palaeontologist, Cincinnati, No. 7, 
 April 16,1883. 
 
 Tracks of Crustacean (?), pi. 2, fig. 4. 
 
 Johnstrup (Fr.) Oversigtover de paleo* 
 zoiske Dannelser paa Bornholm meddelt 
 paa det llte Skaudinaviske Natur- 
 forskermede i Kjobenhavn, 1873, p.299. 
 
 Jones (T. Rupert). On Permian Ento- 
 mpstraca. 
 
 In Monograph of Permian Fossils of Eng- 
 land (King), Palaeont. Soc. London, vol. 3, 
 
 • 1849-’54,p. 58. 
 
 Cythere. 
 
VOGDKS.J 
 
 LIST OF AUTHORS. 
 
 39 
 
 Jones (T. Rupert)— Continued. 
 
 Notes on tbe Entomostraca. 
 
 In Quart. Jour. Geol. Soc. London, vol. 9, 
 1853, p. 160, pi. 7, figs. 5-7. 
 
 Beyrichia. 
 
 This article forms Appendix D to a paper on 
 the Carboniferous and Silurian formations of 
 the neighborhood of Bussaco, in Portugal, by 
 Senhor Carlos Ribeiro, with notes and a de- 
 scription of the animal remains by D. Sharpe, 
 T. W. Salter, and T. R. Jones, etc. See same 
 journal, p. 135, pis. 7-9. 
 
 Notes on tlie Palaeozoic bivalved 
 
 Entomostraca. No. 1. Some species 
 from the Upper Silurian limestone of 
 Scandinavia. 
 
 In Annals Mag. Nat. Hist., 2d series, Lon- 
 don, vol. 16, 1855, p. 81, pi. 5. 
 
 Beyrichia. 
 
 Notes on Palaeozoic bivalved Ento- 
 mostraca. No. 2. Some British and for- 
 eign species of Beyrichia. 
 
 In Annals Mag. Nat. Hist., 2d series, Lon- 
 don, vol. 16, 1855, p. 163, pi. 6. 
 
 Beyrichia. 
 
 ■ Notes on Palaeozoic bivalved Euto- 
 
 mostraca. No. 3. Some species of Leper- 
 ditia. 
 
 In Annals Mag. Nat. Hist., 2d series, Lon- 
 don, vol. 17, 1856, p. 81, pis. 6-7. 
 
 Leperditia. 
 
 Notes on the Palaeozoic bivalved 
 
 Entomostraca. No. 4. North American 
 species. 
 
 In Annals Mag. Nat. Hist., 3d series, London, 
 vol. 1, 1858, p.244, pis. 9, 10. See, also, Rogers’s 
 Final Rept. Geol. Survey Pennsylvania, 1858, 
 pt. 2, p. 834, figs. 695-699. 
 
 Additional notes on Palaeozoic Ento- 
 mostraca from Canada. 
 
 In Annals Mag. Nat. Hist., 3d series, London, 
 vol. 1, 1858, p. 340. 
 
 Leperditia , Isochilina. 
 
 On the Palaeozoic Entomostraca of 
 
 Canada. 
 
 In Geol. Survey Canada, figure and descrip- 
 tion of Canadian organic remains, decade 3, 
 Montreal, 1858, p. 91, pi. 2; also Annals Mag. 
 Nat. Hist., 3d series, London, vol. 1, 1858, p. 244, 
 
 pi. 9. 
 
 . Beyrichia , Leperditia , Isochilinia n. g., Cy- 
 
 theropsis. 
 
 Explanation map 32. The geology 
 
 of the neighborhood of Edinburgh, by 
 H. II. Howell and A. Geikie ; with ap- 
 pendix and list of fossils, by J. W. 
 Salter. 
 
 In Mem. Geol. Survey Gt. Brit., London, 1861, 
 p. 137, pi. 2, fig. 5. 
 
 Jones (T. Rupert)— Continued. 
 
 Prof. T. Rupert Jones herein uses the name 
 of Entomis for certain fossils. For a full ge- 
 neric description, see Annals Mag. Nat. Hist., 
 4th series, London, vol. 11, 1873, p. 413. 
 
 A monograph of the fossil Estherice. 
 
 In Paljcont. Soc. London, vol. 14, 1862, 134 pp., 
 
 5 pis. 
 
 Estheria, Leaia n. g., Beyrichia , Candona, 
 Cypridea. 
 
 Note on Esiheria niddendorjii. 
 
 In Quart. Jour. Geol. Soc. London, vol. 19, 
 1863, p. 73. 
 
 On fossil Esiheria and their distribu- 
 tion. 
 
 In Quart. Jour. Geol. Soc. London, vol. 19, 
 1863, p. 140; also Nat. Hist. Review, 1863, p. 262. 
 
 and Kirkby (J. W.) Notes on the 
 
 Palaeozoic bivalved Entomostraca. No. 
 
 5. 
 
 In Annals Mag. Nat. Hist., 3d series, London, 
 vol. 15, 1865, pi. 20, p. 404. 
 
 Leperditia, Gytherella, Bairdia, Cythere. 
 
 and Holl (H. B.) Notes on the Pa- 
 laeozoic bivalved Entomostraca. No. 6. 
 
 In Annals Mag. Nat. Hist., 3d series, London, 
 vol. 15, 1865, p. 414, pi. 13. 
 
 Primitia n. g. 
 
 and Kirkby (J. W.) Notes on Pa- 
 laeozoic bivalved Entomostraca. No. 7. 
 
 In Annals Mag. Nat. Hist., 3d series, London, 
 vol. 18, 1866, p. 32. 
 
 Entomoconchus, Daphnia, Bairdia, Cythere. 
 
 and Holl (W. B.) Notes on Palaeo- 
 zoic bivalved Entomostraca. No. 8. 
 Some Lower Silurian species from Chair 
 of Kildare, Ireland. 
 
 In Annals Mag. Nat. Hist., 4th series, Lon- 
 don, vol. 2, 1868, p. 54, pi. 7. 
 
 Primitia, Cythere, Bairdia. 
 
 and Holl (H. B.) Notes on Palaeo- 
 zoic bivalved Entomostraca. No. 9. 
 
 In Annals Mag. Nat. Hist., 4th series, Lon- 
 don, vol. 3, 1869, p. 211, pis. 14, 15. 
 
 Cythere, Bairdia, Beyrichia , Primitia, Thlip- 
 sura n. g., p. 213; Cytherellina n. g., p. 215; 
 Kirkby a n. g , Movea n. g., JEchmina n. g., p. 
 217. 
 
 On ancient Water-fleas of the Ostra- 
 
 codous and Phyllopodous tribes (bi- 
 valved Entomostraca). 
 
 In Month. Microsc. Jour., vol. 4, London, 
 1870, p. 184, pi. 61. 
 
 Leperditia, Bairdia, Thlipsura , Cythere, Gy - . 
 therelta, Cytherellina, JEchmina, Carbonia, Oy- 
 pridina, Cypridella, Cyprella , Entomoconchus, 
 Entomis, Primitia, Kirkbya, Moorea, Jsochili- 
 nia, Beyrichia, Leaia, Esiheria. 
 
[BULL. 63. 
 
 40 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Jones (T. Rupert) — Continued. 
 
 On some bivalved Entomostraca j 
 
 from the Coal Measures of South Wales. 
 In Geol. Mag., vol. 7, 1870, p. 214, pi. 9. 
 Cytheroid Entomostraca. 
 
 On the Palaeozoic bivalved Ento- 
 mostraca. 
 
 In Proc. Geologist Assoc., 1870. 
 
 Note on the Entomostraca from the 
 
 Cambrian rocks of St. David’s. 
 
 In Quart. Jour. Geol. Soc. London, vol. 28, 
 
 1872, p. 183, pi. 5. 
 
 Leperditia, Entomis. Larval trilobite ? 
 
 This paper forms a part of Henry Hicks’s ar- 
 ticle on some un described fossils from the Me- 
 nevian Group. Same Jour., p. 173. 
 
 Notes on the Palaeozoic bivalved En- 
 tomostraca. No. 10. 
 
 In Annals Mag. Nat. Hist., 4th series, Lon- 
 don, vol. 11, 1873, p. 413. 
 
 Entomis, Entomidella n. g. 
 
 — On some bivalved Entomostraca, 
 chiefly Cypridenidae of the Carbonifer- 
 ous formations. 
 
 In Quart. Jour. Geol. Soc. London, vol. 29, 
 
 1873, p. 409. 
 
 Sulcuita n. g., Cyprella. 
 
 Ancient Water-fleas, etc. Pt. 2. 
 
 In Monthly Microsc. Jour., vol. 10, London, 
 
 1873, p. 71. 
 
 Cythere, Thlipsura. 
 
 Notes on some forms of British Ento- 
 mostraca from the Silurian rocks of 
 Peeblesshire. 
 
 In Trans. Edinburgh Geol. Soc., vol. 2, pt. 3, 
 
 1874, p. 321. 
 
 Beyrichia, Bairdia, Entomis. 
 
 , Kirkby (J. W.) and Brady (M. P.) 
 
 Monograph of British fossil bivalve 
 Entomostraca from the Carboniferous 
 formations. 
 
 In Palaeont. Soc. London, 1874. 
 
 Pt. 1. The Cypridinadse and their allies, 5 pis 
 Cypridina, Asterope, Philomedes , Bradycine- 
 tus, Eurypylus, Conchcecia, Halocyris , Hetero- 
 desmus , Polycope, Cytherella, Cypridinella n.g., 
 Cypridellina n. g., Gypridella, Sulcuna, Cyprella, 
 Bhombina n. g., Entomoconchus, Off a n. g., 
 Chadocopa, Platycopa. 
 
 aud Kirkby (J. W.) Notes on the 
 
 Palaeozoic bivalved Entomostraca. No. 
 
 11 . 
 
 In Annals Mag. Nat. Hist., 4th series, Lon- 
 don, vol. 15, 1875, p. 52, pi. 6. 
 
 Beyrichia, Leperditia, Primitia, Bairdia, Cy- 
 there. Cytherella. 
 
 Notes on some fossil bivalved Ento- 
 mostraca. 
 
 In Geol. Mag., decade 2, vol. 5, 1878, p. 100, pi. 3. 
 Esther e, Cypris, Candona, Gypridia. 
 
 Jones (T. Rupert) and Kirkby (J. W.) 
 Description of the species of the Ostra- 
 codous genus Bairdia McCoy, from the 
 Carboniferous strata of Great Britain. 
 
 In Quart. Jour. Geol. Soc. London, vol. 35, 
 1879, p. 565, 5 pis. 
 
 Notes on the Palaeozoic bivalved 
 
 Entomostraca. No. 12. Some carbonif- 
 erous species belonging to the genus 
 Carbonia Jones. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 4, 1879, p. 28, pis. 2 and 3. 
 
 Carbonia n. g. 
 
 Notes on the Palaeozoic Entomos- 
 traca. No. 13. Entomis serrato- striata 
 and others of the so-called Cypridinen 
 of the Devonian schist of Germany. 
 
 In Annals Mag. Nat. Hist , 5th series, Lon- 
 don, 79, p. 182, pi. 11. 
 
 Notes on some Palaeozoic Entomos- 
 traca. 
 
 In Geol. Mag., decade 3, vol. 8, 1881, p. 337, 2 
 pis. 
 
 Cypridina ?, Cyprosis, Leperditia?, Entomis, 
 Primitia, Beyrichia, Cyprosina n. g., Polycope. 
 
 Notes on some Palaeozoic Entomos- 
 traca. No. 14. Some Cambrian and 
 Silurian Leperditia and Primitia. 
 
 In Annals Mag. Nat. Hist , 5th series, Lon- 
 don, vol. 8, 1881, p. 332, pis. 19, 20. 
 
 and Schmidt (F.) On some Silu- 
 rian Leperditia. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 9, 1882, p. 168. 
 
 Notes on some Palaeozoic bivalved 
 
 Entomostraca. No. 15. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 10, 1882, p. 358, figs. 1 a, b. 
 
 Primitia. 
 
 Notes on the Palaeozoic bivalved 
 
 Entomostraca. No. 16. 1. Some Palaeo- 
 zoic and other bivalved Entomostraca 
 from Siberian Russia, pi. 6. 2. Some 
 
 Palaeozoic bivalved Entomostraca from 
 Spitzbergen, pi. 9. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 12, 1883, p. 243, pls.6 and 9. 
 
 Entomis, Leperditia, Estheria, Primitia. 
 
 Notes on the late Mr. Tate’s speci- 
 mens of the Lower Carboniferous Ento- 
 mostraca from Berwickshire, North- 
 umberland. 
 
 In Proc. Berw. Nat. Club, vol. 10, 1884, 1 pi. 
 
 Candona ?, Bemix, Carbonia, Macrocypsisf , 
 Leperditia, Beyrichia, Kirkby a, Cythere, Cythe- 
 rella, Estheria, DarvnneUa ?. 
 
VOGDES.] 
 
 LIST OF 
 
 Jones (T. Rupert) — Continued. 
 
 Notes on the Palaeozoic bivalved 
 
 Entomostraca. No. 17. Some North 
 American Leper ditia and allied forms. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 14, 1884, p. 339. 
 
 Leperditia, Isochilina, Primilia. 
 
 Report of the committee, consisting 
 
 of Mr. R. Etheridge, Dr. H. Woodward, 
 and Prof. T. Rupert Jones (secretary), 
 on the fossil Phyllopoda of the Palaeo- 
 zoic rocks. 
 
 In Kept. 53d Meeting Brit. Asso. Adv. Sci., 
 
 1883, p. 215. 
 
 Hymenocari8, Garyocaris, Lingulocaris. 
 
 Second report of the committee con- 
 sisting of Mr. R. Etheridge, Dr. H. 
 Woodward, and Prof. T. Rupert Jones 
 (secretary), on the fossil Phyllopoda of 
 the Palaeozoic rocks. 
 
 In Kept. 54th Meeting Brit. Assoc. Adv. Sci., 
 
 1884. p. 75; Geol. Mag., n. s., decade 2, vol. 10, 
 1883, p. 461. 
 
 and Kirkby (J. W.) On some Car- 
 boniferous Entomostraca from Nova 
 Scotia. 
 
 In Geol. Mag., n. s., decade 3, vol. 1, 1884, p. 
 356, pi. 12. 
 
 Leperditia , Beyrichia, Carbonia, Candona ?, 
 Cythere, Estheria, Leaia, Primitia or Beyrichia. 
 
 and Woodward (Henry). On some 
 
 Palaeozoic Phyllopoda. 
 
 In Geol. Mag., n. s., decade 3, vol. 1, 1884, p. 
 348. 
 
 Discinocaris , Spathiocaris, Pholadocaris, Lis- 
 gocaris, Ellipsocaris. Cardiocaris, Dipterocaris, 
 Pterocari8, Orescentilla, Aptychopsis, Peltocaris, 
 Pinnocaris. 
 
 Notes on the Palaeozoic bivalved En- 
 
 tomostraca. No. 18. Some species of 
 the Entomididae. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 14. 1884, p. 391, pi. 15. 
 
 Entomis , Bolbozoe, Entomidella. 
 
 and Woodward (Henry). Notes 
 
 on the British species of Ceratiocaris. 
 
 In Geol. Mag., n. s., decade 3, vol. 2, 1885, p. 
 385, pi. 10. Continued, ibid., p. 460. 
 
 Kirkby (J. W.) Notes on Palaeozoic 
 
 bivalved Entomostraca. No. 19. On 
 some Carboniferous species of the Os- 
 tracodous genus Kirkby a. 
 
 In Annals Mag. Nat. Hist., 5tli series, Lon- 
 don, vol. 15, 1885, p. 174, pi. 3. 
 
 and Holl (H. B.) Notes on the 
 
 Palaiozoic bivalved Entomostraca. No. 
 20. On the genus Beyrichia and some 
 
 new Bpecies. 
 
 AUTHORS. 41 
 
 Jones (T. Rupert) and Holl (H. B.)— 
 Continued. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 17, 1886, p. 337, pi. 12. 
 
 Beyrichia , Bollia n. g., Kloedenia n. g. 
 
 Notes on the Palaeozoic bivalved 
 
 Entomostraca. No. 21. On some Silu- 
 rian genera and species. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 17, 1886, p. 403, pis. 13, 14. 
 
 Strepula n. g., Bollia, Placentula n. g., Pri- 
 mitia. 
 
 and Kirkby (J. W.) Notes on the 
 
 distribution of the Ostracoda of the 
 Carboniferous formation of the British 
 Isles. 
 
 In Abstracts Proc. Geol. Soc. London, ses- 
 sion 1885-86, No. 489, p. 86. 
 
 On Carboniferous Ostracoda 
 
 from the Gayton borings, Northamp- 
 tonshire. 
 
 In Geol. Mag., n. s., decade 3, vol. 3, London, 
 1886, p. 248, pi. 7. 
 
 Kirkbya, Bythocypris , Macrocypris, Cythe- 
 rella. 
 
 Notes on the Palaeozoic bivalved 
 
 Entomostraca. No. 22. On some unde- 
 scribed species of British Carbonilerous 
 Ostracoda. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 18, 1886, p. 249, pis. 6-9. 
 
 Bythocypris, Cythere ?, Leperditia, Beyrichia, 
 Primitia?, Beyrichiella?, Kirkbya, Moorea, Cy- 
 therella, Bathocythere, Argillcecia, Aglaia?, 
 Xestoleberis ?, Macrocypris, Carbonia, Bairdia. 
 
 On some fringed and other Os- 
 tracoda from the Carboniferous series. 
 
 In Geol. Mag., n. s., decade 3, vol. 3, London, 
 1886, p. 434, pis. 11, 12. 
 
 Beyrichiopsis n. g., Beyrichiella n. g., Bey- 
 richia. 
 
 On Palaeozoic Phyllopoda. 
 
 In Geol. Mag., n. s., decade 3, vol. 3, London, 
 1886, p. 456. 
 
 Ceratiocaris. 
 
 Notes on the distribution of the 
 
 Ostracoda of the Carboniferous forma- 
 tions of the British Isles. 
 
 In Quart. Jour. Geol. Soc. London, vol. 42, 
 1886, p. 496. 
 
 Beyrichiopsis , Phreatura n. g., Youngia n. g. 
 
 This generic name was used tor a new genus 
 of Tlilobites by Lindstrbm in 1885. 
 
 Note. — Since this paper was read many of the 
 species have been described and figured in the 
 Annals Mag. Nat. Hist, for October, 1886, and 
 in the Geol. Mag. of the same date. Others in 
 tbe Proc. Geologist Assoc., vol. 9, 1886. 
 
 Fourth report of the committee, con- 
 sisting of Mr. Ii. Etheridge, Dr. H. 
 
42 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63. 
 
 Jones (T. Rupert) — Continued. 
 Woodward, and Prof. T. Rupert Jones 
 (secretary), on the fossil Phyllopoda of 
 the Palaeozoic rocks, 1886. 
 
 In Kept. 56th Meeting Brit. Assoc. Adv. Sci., 
 
 1886, p. 229. 
 
 Ceratiocaris , Emmelezoe , Xiphocaris, Physo- 
 car is, Cryptozoe. 
 
 and Kirkby (James W.) A list of 
 
 the genera and species of bivalved En- 
 tomostraca found in the Carboniferous 
 formations of Great Britain and Ireland. 
 With notes on the genera and their 
 distribution. 
 
 In Proc. Geologist Assoc., vol. 9, 1886, p. 495. 
 
 I. Cypridinidse : 1. Cypridina, 2. Cypridi- 
 nella, 3. Cypridellina, 4. Cypridella, 5. Sulcuna, 
 6. Cyprella, 7. JBradycinetus, 8. Philomedes, 9. 
 Rhombina. II. Entomoconchidse : 1. Entomo- 
 conchus, 2. Offa. III. Polycopidae : 1. Polycope. 
 IY. Entomididae: 1. Entomis. V. Cytherel- 
 lidas : 1. Cytherella. YI. Leperditiidae : 1. Le- 
 perditia, 2. Bernix, 3. Beyrichia , 4. Beyrichiella, 
 5. Beyrichiopsis, 6. Eirkbya, 7. Moorea, 8. 
 Phreatura. VII. Cyprididae: 1. Aglaia , 2. 
 Candona, 3. Argillcecia, 4. Macrocypris, 5. By- 
 thocy prise .6. Bairdia. VIII. Dawmulidse: 1. 
 Daivinula. IX. Cytheridas: 1. Cythere , 2. 
 Xestoleberis , 3. Bythocythere, 4. Carbonia, 5. 
 Youngia. 
 
 , Etheridge ( R. ) and Woodward 
 
 (H.) Fifth report of the committee, 
 consisting of Mr. R. Etheridge, Dr. H. 
 Woodward, and Prof. T. Rupert Jones 
 (secretary), on the fossil Phyllopoda of 
 the Palaeozoic rocks, 1887. 
 
 In Kept. 57th Meeting Brit. Assoc. Adv. Sci., 
 
 1887, p. 60. 
 
 Ceratiocaris, Dithyrocaris, Leaia, Estheria. 
 
 Notes on the Palaeozoic bivalved 
 
 Entomostraca. No. 23. On some Silu- 
 rian genera and species (continued). 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 19, 1887, p. 117, pis. 4-7. 
 
 Macrocypris, Pontocypris, Bythocypris, Cy- 
 there, CytliereUa , Primitia. 
 
 Prof. T. Kupert Jones remarks in this paper : 
 “Now that not only Cythere hut its allied 
 genera have been fully elucidated in the living 
 state, it is found that the genus does not com- 
 prehend many of the fossil forms once referred 
 to it. Whether these really belong to the 
 Cytheridce or to the Cyprididae it is often diffi- 
 cult to say ; hut the genus Cythere comprises 
 very few of the smooth suhovate forms, and 
 none that have toothless hinges. Hence we 
 find that a real Cythere is scarcely known in 
 Paheozoic strata.” 
 
 Notes on the Palaeozoic bivalved En- 
 tomostraca. No. 24. On some Silurian 
 genera and species (continued). 
 
 Jones (T. Rupert) — Continued. 
 
 In Annals Mag. Nat. Hist., 5th series, Lon- 
 don, vol. 19, 1887, p. 400, pis. 12, 13. 
 
 Thlipsura, Octonaria n. g., Bollia, Primitia, 
 Moorea, Xestoleberis, Achmina. 
 
 Notes on some Silurian Ostracoda 
 
 from Gothland. Stockholm, 1887, 8 pp. 
 
 Beyrichia, Leperditia, Primitia, Primitiopsis 
 n. g., Macrocypris, Bythocypris . Thlipsura, Ach- 
 mina, Bursulella n. g. 
 
 Notes on the Palaeozoic bivalved En- 
 tomostraca. No. 25. On some Silurian 
 Ostracoda from Gothland. 
 
 In Annals Mag. Nat. Hist., 6th series, Lon- 
 don, vol. 1, 1888, p. 395. 
 
 Beyrichia, Leperditia, Entomis, Primitia, 
 Primitiopsis n. g., Macrocypris, Bythocypris, 
 Thlipsura, Achmina, Bursulella n. g. 
 
 Notes on the Palaeozoic bivalved En- 
 tomostraca. No. 26. On some new De- 
 vonian Ostracoda, with a note on their 
 geological position, by the Rev. G. F. 
 Whidborue. 
 
 In Annals Mag. Nat. Hist., 6th series, Lon- 
 don, vol. 2, 1888, p. 295, 1 pi. 
 
 Kyamodes n. g. 
 
 and Woodward (Henry). A mono- 
 graph of the British Palaeozoic Phyllo- 
 poda (Phyllocarida, Packard). 
 
 In Palaeont. Soc. London, vol. 41, 1887, pt. 1. 
 
 Ceratiocaridce. 
 
 On some Scandinavian Phyllo- 
 
 caridaB. 
 
 In Geol. Mag., n. s., decade 3, vol. 5, London, 
 1888, p. 97, pi. 5. 
 
 Ceratiocaris. 
 
 and others. Sixth report of the com- 
 mittee, consisting of Mr. E. Etheridge, 
 Dr. H. Woodward, and Prof. T. Rupert 
 Jones (secretary), on the fossil Phyllo- 
 poda of the Palaeozoic rocks, 1888. 
 
 In Kept. 58th Meeting Brit. Assoc. Adv. Sci., 
 
 1888. 
 
 Ceratiocaris, Echinocaris, Equisitides, Ely- 
 mocaris, Tropidocaris, Mesothyra, Dithyrocaris, 
 Rhinocaris, Spathiocaris, Dipterocaris, Esthe- 
 ria, Hymenocaris, Saccocaris, Lingidocaris, 
 Bactropus, Schizodiscus. 
 
 Author’s edition, 9 pp. and 9 wood-cuts. 
 
 and Woodward ( Henry ). See 
 
 Woodward (Henry) and Jones (T. 
 Rupert). 
 
 See Schmidt (Fr.) and Jones (T. 
 
 Rupert). 
 
 Jordan (H.) Ueberreste eines kleinen 
 iiberaus merkwiirdigen Crustacees. 
 
VOGDES.] 
 
 LIST OF AUTHORS. 
 
 43 
 
 Jordan (H.) — Continued. 
 
 In Yerhandl. natur. Vereins preussischen 
 Rheinlande, Jahrg., vol. 4, 1847, p. 89, pi. 2, 
 figs. 1, 2. 
 
 Gampsonyx (von Meyer) n. g. 
 
 and Meyer (H. yon). Ueber die 
 
 Crustaceen der Steinkoblenformation 
 von Saarbriicken. Cassel, 1854, 2 pis. 
 
 Gampsonyx, Adelophthalmus (Eurypterus), 
 Chonionotus, Arthropleura. 
 
 Jukes (F.) and Sowerby (J. D. C.) An 
 account of a new species of Trilobite 
 found in the Barr limestone in the 
 neighborhood of Birmingham, by Fred- 
 erick Jukes, with a note by J. D. C. 
 Sowerby. 
 
 In Mag. Nat. Hist. (London), vol. 2, London, 
 1829, p. 41, 5 figs. ; Am. Jour. Sci., 1st series, 
 vol. 23, 1833, p. 203; Nenes Jahrbuch fur Mi- 
 neral., 1833, p. 624. 
 
 ( Bumastes barriensis), Asaphus , Calymene. 
 
 Karsten (Gustav). Die Versteiuerungen 
 des Uebergangs-Gebirges in den Ge- 
 rollen der Herzogthumer Schleswig und 
 Holstein. Kiel, 1869, 25 pis. 
 
 Olenu8. Proetu8, Cyphaspis , Phacops, Caly- 
 rnene, Lichas, Trimicleus, Ampyx, Asaphus, 
 Isotelus, Cerauru8, Sphcerexochus, Encrinurus, 
 Nileus, Agnostus, Beyrichia, Cy there. 
 
 Kayser (Emanuel). Beitrage zur Geolo- 
 gie und Paheontologie der Argentini- 
 schen Republik. Cassel, 1876, 2 pis. 
 
 Olenus. Arionellus, Bathyurus?, Arethusina, 
 Ampyx , Asaphus, Ogygia, Agnostus , Leperditia. 
 
 Die Fauna der altesten Devonbildun- 
 
 gen des Harzes. 
 
 In Abhandlungen zur geologisctafcn Special- 
 karte von Preussen und den thuringischen 
 Staaten. Vol. 2, pt 4. Berlin, 1878. Atlas, 36 
 pis. 
 
 Harpe8, Proelus, Cryphceus, Cyphaspis , Pha- 
 cops , Dalmanites , Lichas, Acidaspis , Bronteus, 
 Primitia, Dithyrocaris. 
 
 Ueber Dalmanites rhenanus , eine Art 
 
 der HaMsmanni-Gruppe, und einige au- 
 dere Trilobiten aus den alteren rhei- 
 nischen Dachschiefern. 
 
 In Zeitscbr. Deutscb. geol. Gesell., vol. 32, 
 1880, p. 19, pi. 3. 
 
 Phacops, Cryphceus , Dalmanites. 
 
 Dechenella, eine devonische Gruppe 
 
 der Gattung Phillipsia. 
 
 In Zeitschr. Deutsch. geol. Gesell., vol. 32, 
 1880, p. 703, pi. 27. 
 
 Dechenella n. g. 
 
 Beitrage zur Kenntniss von Oberde- 
 
 von und Culm am Nordrande des rhei- 
 nischen Schiefergebirges; Arten aus 
 dem Culm von Aprath. 
 
 Kayser (Emanuel) — Continued. 
 
 In Jahrbuch Preuss. geol. Landesanst. und 
 Bergakad., Berlin, 1881, p. 67. 
 
 Phillipsia cequalis, P. longicornis, P. eich- 
 waldi, P. emarginata. 
 
 Die Orthocerasschiefer zwischen 
 
 Balduinstein und Laurenberg an der 
 Lahn. Palaeontologischer Anhang. 
 
 In Jahrbnch Preuss. geol. Landesanst. und 
 Bergakad., Berlin, 1883, p. 34, pi. 3, fig. 6. 
 
 Phacops fecundus, Cryphceus rotundi/rons , , 
 C. kochi. 
 
 Mittel- und obersilurische Verstei- 
 uerungen aus dem Gebirgsland von 
 Tshau Tiens. 
 
 In Chipa (Richthofen), vol. 4, Berlin, 1883, 
 p. 37. 
 
 Asaphxis, Calymene, Trinucleus richthofeni, 
 Encrinurus. 
 
 Obercarbonische Fauna von Loping. 
 
 In China (Richthofen), vol. 4, Berlin, 1883, p. 
 161. 
 
 Phillipsia obtusicauda , pi. 19, fig. 3. 
 
 Keyes (Chas. R.) On the fauna of the 
 Lower Coal Measures of central Iowa. 
 
 In Proc. Acad. Nat. Sci. Phila., 1888, p. 222. 
 
 Cythere nebracensis. 
 
 Kiesow (J. von). Ueber silurische und 
 devonische Geschiebe West-Preussens. 
 
 In Schrift. nat. Gesell. Danzig, new series, 
 vol. 6, 1884, p. 205, 3 pis. 
 
 Proetus, Phacops, Calymene, Lichas, Ampyx, 
 Asaphus, Ptychopyge, Illoenus. Acidaspis, 
 Cheirurus, Encrinurus, Beyrichia, Leperditia, 
 Primitia, Cytherellina. 
 
 Ueber gotlandische Beyrichien. 
 
 In Zeitschr. Deutsch. geol. Gesell., vol. 40, 
 1888, p. 1, 2 pis. 
 
 Kinnear ( W. T. ) Note on the occurrence 
 of a new Carboniferous Crustacean at 
 Ardrois Castle, Fife. 
 
 In Trans. Edinburgh Geol. Soc., vol. 5, pt. 3, 
 1887, p. 417. 
 
 Dithyrocaris, Palceocrangon, Ceratiocaris, 
 Rostrocaris n. g. 
 
 Kinsky (Gra/ von). Schreiben des H. 
 Grafen von Kinsky an von Born iiber 
 einige mineralogische und lithologische 
 Merk wiirdigkeiten . 
 
 In Abhandlungen einer Privat-Gesell. in Boh- 
 men, vol. 1, Prag, 1775, p. 243. 
 
 Kirkby ( J. W. ) On some Permian fos- 
 sils from Durham. 
 
 In Trans. Tyneside Nat. Field Club, vol. 3, 
 1858, p. 286. 
 
 On Permian Entomostraca from the 
 
 shell limestone of Durham. With notes 
 on the species by T. Rupert Jones. 
 
44 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 Kirkby (J. W.)— Continued. 
 
 In Annals Mag. Nat. Hist., 3d series, Lon- 
 don, vol. 2, 1858, p. 317, 4 pis. 
 
 Kirkbya, Gytheridce, Cythere, Bairdia. 
 
 — - and Jones (T. Rupert). On Per- 
 mian Entomostraca. 
 
 In Trans. Tyneside Nat. Field Club, vol. 4, 
 1859, p. 122, 4 pis. 
 
 See, also, Jones (T. Rupert) and Kirkby (J. 
 W.), and Jones (T. Rupert), Kirkby (J. W.), 
 and Brady (M. P.). 
 
 On the Permian rocks of Sou tli York- 
 shire and their Palaeontological rela- 
 tions. 
 
 In Quart. Jour. Geol. Soc. London, vol. 17, 
 1861, p. 287. 
 
 Cythere (Bairdia), Kirkbya. 
 
 On some additional species that are 
 
 common to the Carboniferous and Per- 
 mian strata. 
 
 In Annals Mag. Nat. Hist., 3d series, Lon- 
 don, vol. 10, 1862, p. 202. 
 
 Kjerulf (Theo. ) Yeiviser ved geologiske 
 Exkursioner i Christiania og Omegn. 
 Christiania, 1865. 
 
 The author herein gives a list of Norwegian 
 Silurian fossils, with some notes and figures on 
 the genera Ceratopyge, Cyrtometopus, Illcenus, 
 Phacops. 
 
 Klein (J. T.) Specimen descriptionis 
 petrefactorum Gedanensium order Ory c- 
 tographia Gedannensis, etc. (*) 
 
 In Nuremberg, 1770, folio, pi. 15, figs. 5-7. 
 
 Calymene blumenbachii. 
 
 Kloden (K. F.) Die Yersteinerungen des 
 Mark Brandenburg, etc. Berlin, 1834, 
 10 pis. 
 
 Cytherina phaseolus Calymene blumen- 
 bachii, C. var . tuber culata, C. var .pulchella, C. 
 sclerops, C. punctata, C. concinna, C.polytoma?, 
 Asaphus extenuatus? , A. angustifrons, A. ex - 
 pansus, A. auriculatus, A. dilatatus, A. (I lice- 
 nus) crassicauda, A. ( Ampyx ) nasutus?, A.cau- 
 datus, Battus pisiformis, B. tuberculatus, pi. 1, 
 figs. 16-23. F. McCoy, “Brit. Pal. Rocks,” p. 
 135, remarks on this species that the name Bey- 
 richia tuberculatus is generally applied to fig. 
 22 of Kloden’s plate, which is a common form 
 in the Gothland beds) ; Battus gigas, pi. 2, fig. 1. 
 
 Koch (C.) Monographie der Homalo- 
 notus-Arten des rheinischen Unterde- 
 von. 
 
 In Preuss. geol. Landesanstalt, Abhandl., 
 Berlin, 1883, vol. 4, pt. 2. 
 
 Koenen (A. von). Die Kulm-Fauna von 
 Herborn. 
 
 In Neues Jahrbuch fur Mineral., 1879, p. 309, 
 pis. 6, 7. 
 
 Phillipsia, Proetus. 
 
 Koenen (A. von) — Continued. 
 
 Ueber die Unterseite der Trilobiten. 
 
 In Neues Jahrbuch fiir Mineral., 1880, vol. 1, 
 p. 429, pi. 8, figs. 9, 10. 
 
 Phacops, Asaphus, Calymene. 
 
 Ueber Clymenienkalk und Mittel- 
 
 Devonien bei Montpellier. 
 
 In Neues Jahrbuch fiir Mineral., 1886, p. 163. 
 
 Deckenella escoli. 
 
 Kolmodin (Lars). Bidrag till kaune- 
 domen om Sveriges Siluriska Ostra- 
 coder. 
 
 In Akad. Afhandling som med tillstand af 
 Tidtberomda Filosofiska Fakultetens i Upsala, 
 etc., 1869, 1 pi. 
 
 Leperditia, Beyrichia, Gytheropsis, Pipe. 
 
 Ostracoda Silurica Gotlandise enu- 
 
 merat. 
 
 In Ofversigt kongl. Vet. Akad. Forhandlin- 
 gar, 1879, No. 9, p. 133, pi 19. 
 
 Leperditia, Beyrichia, Elpe. 
 
 Konig (C. E.) leones fossilium sectiles. 
 
 Centuria prima, text, 4 pp., pis 1-8; Cen- 
 turia seconda, pis. 9-19. ; n. d. 
 
 The common edition of this work has only 
 four pages of text and eight plates (London, 
 1820, 4to). 
 
 Calymene decipiens, p. 2, pi. 3, fig. 32 (Ellipso- 
 cephalushoffi) ; Asaphus my ops, p. 3, pi. 4, fig. 53; 
 Homalonotus n. g., E. knighti, p.4, pi. 7, fig. 85; 
 Agnostics, pi. 10, figs. 119,120; Isotelus gigas, pi. 
 10, fig. 121; Asaphus extenuatus, pi. 10, fig. 122; 
 
 A. crassicauda, pi. 13, fig. 150; Belinurus n. g., 
 
 B. bellulus] pi. 18, fig. 230. 
 
 For a description of the genus Belinurus, see 
 W. H. Baily’s article, Annals Mag. Nat. Hist., 
 3d series^London, vol. 11, 1863. 
 
 Koninck (L.-G. de). M6moire sur les 
 Crustac&s fossiles de Belgique. 
 
 In Mem. Acad. Sci. Bruxelles, vol. 14, 1841, 
 
 lpl. 
 
 Goldius n. g., Asaphus, Cyclus n. g., Cythe- 
 rina, Cypridina, Cyprella n. g. (Phillipsia and 
 Bronteus). 
 
 Description des animaux fossiles qui 
 
 se trouvent dans le terrain carboui- 
 fere de Belgique. Li&ge, lH42-’44. 
 
 Cythere, Cypridina, Cyprella. Cypridellan. g., 
 Cyclus, Phillipsia brongniarti, P. globiceps, P. 
 derbyensis, P. gemmulifera, P. pustulata, P. 
 jonesii. 
 
 Recherches sur les fossiles palaeo- 
 
 zoiques de la Nouvelle-Galles du Sud 
 Australia. 
 
 In M6m. Soc. Sci. Li6ge, 2d series, voL 6, 1877. 
 
 Jllamus, Staurocephalus, Cheirurus Encri- 
 nurus, Gromus, Calymene, Proetus, Lichas, 
 Bronteus, Harpes. 
 
VOGDE6.] LIST OF 
 
 Koninck (L.-G. de)— Continued. 
 
 Rechcrckes sur les fossiles palseo- 
 
 zo'iques de la Nouvelle-Galles du Sud 
 Australie. 
 
 In M6m. Soc. Sci. Li&ge, 2d series, vol. 7, 1878. 
 
 Phillipsia, Griffithides, Brachymetopus. 
 
 Sur une nouvelle espkce de crustacd 
 
 du terrain houiller de la Belgique. 
 
 In Bull. Acad. Sc. Bruxelles, 2d series, vol. 
 45, 1878, p. 409, 1 pi. 
 
 Brachypyge carbonis. 
 
 The principal part of this article is a letter 
 from Dr. Henry Woodward to L. G. de Koninck. 
 
 Notice sur le Prestwichia rotundata 
 
 J. Prestwick, decouvert daus le sckiste 
 kouiller de Horrae, prks Mona. 
 
 In Bull. Acad. Sci. Bruxelles, 3d series, vol. 1, 
 1881, p. 91, 1 pi. 
 
 Krause (A.) Die Fauna der sogen. 
 Beyrichien oder Ckoneten-Kalke des 
 norddeutscken Diluviums. 
 
 In Zeitschr. Deutsch. geol. Gesell., vol. 29, 
 Berlin, 1877, p. 1, 1 pi. 
 
 Oalymene blumenbachii , Phacops downingce , 
 Proetus concinus, Leperditia , Beyrichia, Cythe- 
 rellina, Primitia. 
 
 Kuntgen (K.) Die Trilokiten. (*) 
 
 In Mus. Luxemburg, 1877. 
 
 Kutorga (S.) Beitrage zur Kenntn. der 
 organiscken Uekerreste des Kupfer- 
 aandst. am westl. Abkange des Urals. 
 St. Petersburg, 1838, p. 22, pi. 4, figs. 
 1-3. 
 
 Limulue oculatus Kutorga. 
 
 Edouard d’Eichwald (‘ Lethma Rossica,” vol. 
 1, p. 1360) uses this species for a type of his new 
 genus, Oompylocephalu8. 
 
 Ueber einige kaltische silurische 
 
 Trilokiten. 
 
 In Verhandl. russ. k. mineral. Gesell. zu St. 
 Petersburg, 1847, p. 287, plate. 
 
 A8aphu8, Ill(enu8 y Bncrinurus. 
 
 Einige Sphcerexochus und Cheirurus 
 
 ana den ailuriscken Kalksteiuschickten 
 dea Gov. St. Petersburg. 
 
 In Verhandl. russ. k. mineral. Gesell. zu St. 
 Petersburg, 1854, p. 105, 3 pis. 
 
 Oheirurus gembnitzkii, O. macrophthahnus, 
 Sphcerexochus cranium, , S. hemicranium, S. 
 platy cranium, S. enurus. 
 
 Lang (C. N.) Hiatoria lapidum figura- 
 torurn Helvetia ej usque viciute in qua 
 enarranturomnia eorurn genera, species 
 et vires. Venetiia, 1708. ( # ) 
 
 Tractatus de origine lapidum figura- 
 
 torum Helvetia. Lucernaj, 1700. (*) 
 
 AUTHORS. 45 
 
 Laspeyres (H.) Das fossile Pkyllopo- 
 den-Genus Leaia. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 1870, p. 733, 1 pi. 
 
 Latreille (P.-A.) Affinit6s desTrilobites. 
 
 In Mem. Mus. Hist. Hat., Bruxelles, vol. 7, 
 1821, p. 22 ; Annals Sci. Phys., Bruxelles, vol. 6. 
 
 Lawrow (N.) Zwei neue Asapkus-Arten 
 aus dem siiuriscken Kalksteine. 
 
 In Verhandl. russ. k. mineral. Gesell. zu St. 
 Petersburg, 1855-56, p. 237, pis. 4, 5. 
 
 Ptycliopyge und Megalaspis, Trilobi- 
 
 ten der unter-siluriscken Kalksteine. 
 
 In Verhandl. russ. k. mineral. Gesell. zu St. 
 Petersburg, 1857-’58, p. 146, plate. 
 
 Lebesconte (M.-P.) Constitution g6u.6- 
 rale du massif breton compares a celle 
 du Finist&re. 
 
 In Bull. Soc. Geol. France, 3d series, vol. 14, 
 1886, p. 776, pis. 34-36. 
 
 Homalonotus barroisi , II. heberti, Ogygites. 
 
 Lehmann ( J. G. ) Versuck einer Ge- 
 schickte von Flotzgebirgen betreffeud 
 deren Entstekung, Lage, darin befind- 
 licken Metalle, Mineralien und Fossi- 
 lien. Berlin, 1756. (*) 
 
 De Entrockis et Asteriis. (*) 
 
 In Hovi Comm. Sci. Petropol., vol. 10, 1764, 
 p. 429, par. 12, par. 12, figs. 8-10. 
 
 Leuchtenberg (M. H. von). Beschrei- 
 bung einiger neuer Tkierreste der Ur- 
 welt von Zarskoje-Selo. St. Peters- 
 burg, .1843, 2 pis. 
 
 Asaphus, Nileus , Metopias. 
 
 Lhwyd (Edward). Part of a letter from 
 Mr. Edward Lkwyd to Doctor Martin 
 Lister. 
 
 In Philos. Trans. Royal Soc. London, vol. 20, 
 No. 243, 1698, p. 299, plate, figs. 8, 9, and 10. 
 
 This paper contains the earliest account of 
 Trilobites. The author discovered two frag- 
 ments and one entire specimen of Ogygia buchii 
 near Llandeilo, in Carmarthenshire. Lhwyd 
 says in his letter that he did not know what to 
 make of these fossils. The Ogygia (fig. 10) he 
 refers to the skeleton of an unknown fish. Fig. 
 8 represents the head of a species of the genus 
 Trinucleus. 
 
 Litkophylacii Britannici Ichnogra- 
 
 phia. Londiui, 1699, 23 pis.; 2d ed., 
 1760. 
 
 This work gives a catalogue of English fos- 
 sils contained in the Ashmolean Museum, and 
 also several essays on fossils. In the author’s 
 article “ Epistolal. delapidibus quibusdam Ger- 
 mania acceptis,” pp. 95-100, he alludes to an 
 Ogygia, and remarks : “ This ichthyomorphous 
 stone swims spread out on its side, although it 
 
46 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Lhwyd (Edward) — Continued. 
 
 does not correspond to any specimen heretofore 
 discovered; it does not agree in its external out- 
 line to your fossil, but represents the skeleton 
 of the same or of a sole, only the specimen is 
 striated on the circumference. The figure be- 
 longs to Buglossium, or the sole fish, except it 
 is somewhat larger and less compressed at its 
 extremities, hut it wants the tail of a fish. We 
 call it Buglossam curtam strigosam." He also 
 gives a description and figure of Trinucleus Jim- 
 briatum vulgare , pi. 22, 23, on which It. I. Mur- 
 chison afterwards founded the genus Trinucleus. 
 
 Lindaker ( T. J. ) Beschreibung einer 
 noch nicht bekannteu Kafermuschel. (*) 
 
 In Mayer’s Sammlung phys. Aufsatze, Dres- 
 den, vol. 1, 1791, p. 37, pi. 1. 
 
 The author describes under the name of 
 “gegitterte Kafermuschel” a Trinucleus from 
 Prague. 
 
 Lindstrom (G.) Norminafossilium Silu- 
 riensium Gotlandiae Laroverks program. 
 Yisby, 1867. 
 
 Proetus, Phacops, Calymene, Homalonotus, 
 Lichas, Acidaspis, Trapelocera, Cheirurus, Dei- 
 phon, Sphcerexochus, Oryptonymus , Bronteus, 
 BumastMS , Eurypterus, Pterygotus, Ceralioca- 
 ri8, Beyrichia , Leperditia, Gytheropsis. 
 
 List of tbe fossils of tbe Upper Silu- 
 rian formation of Gothland. Stock- 
 holm, 1885. 
 
 Forteckning pa Gotland Siluriska 
 
 Crustac^er. 
 
 In Ofversigt. Kongl. Vet. Akad. Forhand- 
 lingar, 1885, No. 6, p. 37, pis* 12-16. 
 
 Harpes, Proetus , Cypkaspis, Phcetonides, Pha 
 cops , Calymene, Homalonotus, Lichas, Trochu- 
 rus, Acidaspis, Cheirurus , Sphcerexochus, Youn- 
 gia n. g , Deiphon, Encrinurus, Illcenus , Bron- 
 teus, Eurypterus. 
 
 Linnarsson (J. G. O.) Om de Siluriska 
 bildningarne i Mellersta Westergot- 
 land. 1. 
 
 In Akad. Afhandling som med tillstand af 
 Vidtberomda Filosofiska Fakulten i Upsala, 
 etc., 1866, 2 pis. 
 
 The Trilobites are .grouped as follows : 
 Phacopidae: Phacops. Cheiruridae: Pliomera, 
 Cyrtometopus, Sphcerexochus. Encrinuridae : 
 Cybele. Acidaspidae: Acidaspis. Lichidae : ££- 
 chas. Harpedidae : Arraphus. Calymenidae : 
 Calymene, Homalonotus. Aulacopleuridae: 
 Aulacopleura. Liostracidae : Liostracus. Ole- 
 nidae : Paradoxides, Olenus, Peltura, Parabo- 
 lina, Eurycare, Sphcerophthalmus. Pemo- 
 pleurideae: Remopleurides. Proetidao: Forbe- 
 sia. Asapliidae: Asaphus, Megalaspis, Pty- 
 chopyge, Ogygiaf, Niobe. Hlaeuidae: Illcenus , 
 Rhodope, Nilcus, Symphysurus, JEglina. Tri- 
 nucleidae: Trinucleus, Ampyx , Lonchodomas, 
 Raphiophorus, Dionide. Aguostidae : Agnos- 
 tus. Incertae sedis: Holometopus. 
 
 Linnarsson (J. G. O.) — Continued. 
 
 The author also gives descriptions and fig- 
 ures of the following species : Phacops pulchel- 
 lus, Cyrtometopus latilobus, Sphcerexochus lati- 
 ceps, Lichas segmentatus, Ogygia? apiculata, 
 Illcenus limbatus, Agnostus ajfinis. 
 
 Om Vestergotlands Cambriska ocb 
 
 Siluriska Aflagringar. 
 
 In Kongl. Svenska Vet.-Akad. Handl., vol. 
 
 8, No. 2, 1869, 2 pis. 
 
 Harpes, Remopleurides, Paradoxides, Dikelo- 
 cephalus, Olenus, Trigrthrus, Ceratopyge, Cono- 
 coryphe, Anomocare, Arionellus, Liostracus, 
 Euloma, Holometopus, Proetus, Harpides, Phil- 
 lipsia, Phacops, Calymene, Homalonotus, Lichas, 
 Trinucleus, Ampyx, Dionide, Asaphus, Mega- 
 laspis, Symphysurus, Stygina, Ogygia, Niobe, ~ 
 AUglina, Acidaspis, Cheirurus, Sphcerexochus, 
 Staurocephalus, Pliomera, Cybele, Encrinurus, 
 Dindymene, Nileus, Panderia, Agnostus, Leper- 
 ditia, Beyrichia, Primitia. 
 
 Diagnoses specierum novarum e 
 
 class© Crustaceorum in depositis Cam- 
 brisis et Siluricis Vestrogotise Sueciae 
 repertarum. 
 
 In Ofversigt. Kongl. Svenska Vet.-Akad. 
 Forhandl., 1869, No. 1, p. 191. 
 
 Remopleurides, Triarthrus, Phacops, Trinu- 
 cleus, Symphysurus, Ogygia, Niobe . Acidaspis, 
 Cheirurus, Cybele, Dindymene, Panderia, Ag- 
 nostus, Lichas i Leperditia, Beyrichia, Primitia, 
 Trilobites cenigma. 
 
 Jemforelse mellan de Siluriska afla- 
 
 gringarne i Dalarne ocb i Yestergot- 
 land. 
 
 In Ofversigt. Kongl. Svenska Vet. -Acad. 
 Forhandl., 1871, No. 3, p. 339. 
 
 Remopleurides, Trinucleus, Proetus, Phacops, 
 Chasmops, Illcenus, Nileus. Beyrichia, Primitia. 
 
 Mere mention of occurrence. 
 
 Om nagra forsteningar fran Sveriges 
 
 ocb Norges “Primordialzon.” 
 
 In Ofversigt Kongl. Svenska Vet.-Akad. For- 
 handl., 1871, No. 6. 
 
 Paradoxides kjerulfi, pi. 16, figs. 1-3. 
 
 Anteckningar om den Cambrisk- 
 
 Siluriska lagerserien Jemtland. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 1, No. 3, 1872, p. 34. 
 
 Ofversigt af Nerikes ofvergangsbild- 
 
 ningar. 
 
 In Ofversigt Kon gl. Svenska V et. - Akad . For- 
 handl.,1875, No. 5, pi. 5; Sveriges Geologiska 
 Undersokning Ser. C, No. 21, 1875. 
 
 Paradoxides, Ellipsocephalus, Leptoplastus 
 n g., Beyrichia. 
 
 Trilobiter frau Vestergotlands An- I 
 
 drarurn kalk. 
 
 In Geol. Foreningens Stockholm Forhandl., j 
 vol. 2, 1875, p. 491. 
 
vogdes.1 LIST OF 
 
 Linnarsson (J. G. O.)— Continued. 
 
 En egendomlig Trilobitfauna fran 
 
 Jemtland. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 2, No. 12, 1875, p. 491, pi. 22, figs. 1-5. 
 
 IHeelloceji^alus billing si, Triarthrus jemt- 
 landicus, Remopleurides microphthalmus, Bohe- 
 millaO ) denticulata. 
 
 Tva nya Trilobiter fran Skanes 
 
 alumskiffer. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 2, No. 12, 1875, p. 498. 
 
 Liostracus (?) superstes, Cyclognathus n. g., 
 O. micropygus. 
 
 Geologiska iakttagelser under en 
 
 resa pa Oland. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 3, No. 2, 1876, p. 71. 
 
 Om faunan i lagren med Paradoxides 
 
 olandicus. 
 
 In SverigesGeologiska Undersokning, Ser. C, 
 No. 22, 1877, 2 pis. 
 
 Paradoxides, Ellipsocephalus , Gonocoryphe , 
 Agnostus. 
 
 Om de palseozoiskabildningarna vid 
 
 Humlenas. 
 
 In Sveriges Geologiska Undersokning, Ser. 
 C, No. 28, 1878. 
 
 On the Trilobites of the Shineton 
 
 shales. 
 
 In Geol. Mag., new series, decade 2, vol. 5, 
 1878, p. 188. 
 
 Gonocoryphe, Remopleurides. 
 
 Om faunan i kalken med Gonocoryphe 
 
 exsultans. 
 
 In Sveriges Geologiska Undersokning, Ser. 
 C, No. 35, 1879, 3 pis. 
 
 Paradoxides, Liostracus, Solenopleura, Gono- 
 coryphe, Agnostus. 
 
 ■ Ceratopygekalk och undre grapto- 
 
 litskiffer p& Falbygden, i Vestergot- 
 land. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 4, 1879, p. 269. 
 
 Om forsteningarne i de Svenska 
 
 lagren med Peltura och Sphserophthal- 
 mus. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 5, 1880, No. 4; Sveriges Geologiska Under- 
 sokning, Ser. C, No. 43, 1880. 
 
 Peltura, Sphcerophthalmus, Anopocare, Cte- 
 nopyge n. g., Agnostus. 
 
 Promemoria lemnad af A. G. Na- 
 
 thorst for resa pa Oland. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 5, No. 13, 188L 
 
 De undre Paradoxides lagren vid 
 
 Andrarum. 
 
 In Sveriges Geologiska Undersokning, Ser. 
 C, No. 54, 1883, 4 pis. 
 
 AUTHORS. 47 
 
 Linne (C.) Olandska och Gotlandska 
 resa. Stockholm och Upsal, 1715. 
 
 On p. 147, under the name of Entomolithus 
 paradoxus, there is in this work a rough wood- 
 cut of the pygidium of Asaphus expansus Linn. 
 
 Wastgdta resa forrattad ar 1746. 
 
 Stockholm, 1747. 
 
 On pp. 87 and 88 of this work there are some 
 rough wood-cuts of Trilobites, probably an 
 Olenus and the head of a Paradoxides. 
 
 Museum Tessinianum. Holmise, 
 
 1753, p. 123, pi. 3. 
 
 Entomolithus, pi. 3, fig. 2 ( Galymene tubercu- 
 latus ): E. paradoxus, pi. 3, fig. 1 ( Paradoxides 
 tessini). 
 
 Skanska resa. Stockholm, 1757, p. 
 
 121 . 
 
 Petrificatet Entomolithus paradoxus 
 
 beskrifed. 
 
 In Acta Regiae Acad. Sci. Holmiens., vol. 21, 
 1759, p. 19, pi. 1, figs. 1-4. 
 
 Entomolithus paradoxus, pi. 1, fig. 1 ( Olenus 
 spinulosus) ; Entom. paradoxus 8 cantliaridum, 
 pi. 1, fig. 4, head ( Olenus gibbosus ) ; Entom. No. 
 3, pi. 1, fig. 3 ( Galymene blumenbachii) ; Entom. 
 No. 2, pi. 1, fig. 2 (Encrinurus punctatus) . 
 
 Systema natures. Ed. 12. Vol. 3. 
 
 Holmise, 1768, p. 160. 
 
 Entomolithus paradoxus a expansus (Asa- 
 phus expansus Linn.). E. paradoxus p canthari- 
 dum ( Olenus gibbosus "Wahl.), E. paradoxus y 
 pisiformis (Agnostus pisiformis Linn.). 
 
 Littleton (Charles). On a nondescript 
 petrified insect. 
 
 In Philos. Trans. Royal Soc. London, vol. 46, 
 No. 496, 1750, p. 598, pi. 1, figs. 3-12, pi. 2. 
 
 Galymene blumenbachii. 
 
 Locke (John). On Isotelus maximus , 
 found near Trebers, in Adams County, 
 Ohio. 
 
 In Second Ann. Rept. Geol. Survey Ohio (W. 
 W. Mather), 1838, p. 247, fig. 8. 
 
 On a new species of Trilobite of very 
 
 large size. 
 
 In Trans. Assoc. Am. Geol. and Naturalists, 
 vol. 1, 1843, p. 221, plate. 
 
 Isotelus megistos Locke. 
 
 Dr. John Locke has herein given a new name 
 to the species which he called Isotelus maxi- 
 mus in the Second Ohio Report. See, also, Am. 
 Jour. Sci., 1st series, vol. 42, 1843, p. 366, 1 pi. 
 
 Notice of a new Trilobite. 
 
 In Am. Jour. Sci., 1st series, vol. 44, 1843, p. 
 346. 
 
 Geraurus crosotus. 
 
 Supplementary notice of the Cerau- 
 
 ru8 crosotus. 
 
 In Am. Jour. Sci., 1st series, vol. 45, 1843, p. 
 223. 
 
A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 48 
 
 liogan (W. E.) Bronteus canadensis. 
 
 In Kept. Geol. Survey Canada, 1844, p. 54, 2 
 figs. 
 
 On the tracks of an animal lately 
 
 found in the Potsdam sandstone. 
 
 In Canadian Naturalist, vol. 5, 1860, p. 279. 
 
 Lossen (K. A.) Ueber Cryphceus rotundi- 
 frons aus dem zorger Schiefer des 
 siidlichen Unterharzes. 
 
 In Zeitsebr. Deutsch.xgeol. Gesell., vol. 31, 
 1879, p. 215. 
 
 Cryphceus. 
 
 Loven (S. L.) On Calymene clavifrons 
 and C. ovata. 
 
 InOfversigtKongl. Svenska Vet.-Akad. For- 
 handl.,1845, p. 63. 
 
 Svenska Trilobiter. 
 
 InOfversigt Kongl. Svenska Vet.-Akad. For- 
 handl., 1845, pp. 46, 104, pis. 1, 2. 
 
 Trinucleus, Proetus, Metopias, Lichas, Cerate- 
 ru*, Cybele n. g. 
 
 Lungren (B.) Om den vid Rams&sa och 
 Ofveredskloster i Skane forekommande 
 sandst$nens alder. 
 
 In Acta Univ. Lundensis, 1874. 
 
 Leperditia. 
 
 MacLeay ( W. S. ) Observations on 
 Trilobites, founded on a comparison of 
 their structure and that of living Crus- 
 tacea. 
 
 In R. I. Murchison. ‘ ‘ The Silurian system , ’ ’ 
 London, 1839, p. 666; Annals Mag. Nat. Hist., 
 1st series, London, vol. 4, 1839, p. 16. 
 
 The author compares them with Apus and 
 other Aspidophora, animals which, in his 
 opinion, of all the Entomostraca, appear to come 
 nearest to the Trilobita. 
 
 McCoy (Frederick). On Entomoconchus 
 
 8Conli. 
 
 In Jour. Geol. Soc. Dublin, vol. 11, 1839, p. 91, 
 pi. 5, figs, a, c. 
 
 Entomoconchus n. g. 
 
 A synopsis of the characters of the 
 
 Carboniferous limestone fossils of Ire- 
 land. Dublin, 1844, 29 pis. 
 
 The title-page bears no author’s name. The 
 book shows that it was prepared by Frederick 
 McCoy, under the direction of Richard Griffith, 
 the collector, in whose cabinet all the speciae 
 were contained. 
 
 Phillipsia, OriJJithides, Calymene , Dithyro- 
 caris, Entomoconchus , Cytherina, Bairdia n. g., 
 Cythere, Daphma. 
 
 A synopsis of the Silurian fossils of 
 
 Ireland, collected from the several dis- 
 tricts by Richard Griffith, F. G. S. 
 The whole being named, and the new 
 
 McCoy (Frederick) — Continued, 
 species drawn and described, by Fred- 
 erick McCoy. Dublin, 1846, 5 pis. 
 
 Harpes, Remopleurides, Forbesia n. g., Pha - 
 cops, Portlockia n. g., Calymene, Homalonotus, 
 Lichas, Trinucleus, Ampyx, Ogygia, Isotelus, 
 lllcenus, Acidaspis, Cheirurus, Sphcerexochus, 
 Otarion, Encrinurus, Bronteus, Trinodus u. g., 
 Tiresias n. g., Beyrichia n. g., Cythere, Battus. 
 
 A notice of the new genera described by 
 Frederick McCoy is given in the Ray Society’s 
 edition of Burmeister’s “ Organization of Trilo- 
 bites. Supplementary appendix,” p. 123. 
 
 The generic name Tiresias was used in 1845 
 for a genus of the Coleoptera, and that of 
 Forbesia for one of the Polypi in 1845. Trinodus 
 was used in 1846 for a genus of the Coleoptera. 
 
 On the fossil botany and zoology of 
 
 the rocks associated with the coal of 
 Australia. 
 
 In Annals Mag. Nat. Hist., 1st series, Lon- 
 don, vol. 20, 1847, p. 226, plato. 
 
 Phillipsia, Brachymetopus n. g., Cythere, 
 Bairdia. 
 
 On the classification of some British 
 
 fossil Crustacea, with notices of new 
 forms in the University collection at 
 Cambridge. 
 
 In Annals Mag. Nat. Hist., 2d series, Lon- 
 don, vol. 4, 1849. 
 
 Asaphime: 1. Phacops, 2. Calymene , 3. Tri- 
 merocephalus n. g., 4. Asaphus (subgenera, Iso- 
 letus, Basilicus), 5. lllcenus (subgenera, lllcenus, 
 Bumastus, Dysplanus), 6. Forbesia, 7. Phil- 
 lipsia. Paradoxinse : 1. Paradoxides (subgenus, 
 Olenus), 2. Ceraurus,3. Cryphceus, A Sphcerexo- 
 chus, 5. Acidaspis, 6. Staurocephalus, 7. Remo- 
 pleurides, 8. Zethus. Ogyginm : 1. Trinucleus 
 (subgenus, Tetrapsellium) ', 2. Tretaspis n. g., 3. 
 Ampyx, 4. Ogygia, 5. Bronteus, 6. Lichas (sub- 
 genera, Trochurus, Acanthopyge). Harpedinse : 
 1. Harpes, 2. Harpidella n. g., 3 Amphion. Ag- 
 nostinse : 1. Trinodus, 2. Agnostus, Chasmopsxt. 
 g., Oriffi,thides, Barrandia n. g., Ceratiocaris 
 n. g., Cytheropsis n. g., Pterygotus. 
 
 Partly republished in the author’s “Contri- 
 butions to British Palaeontology, etc.,” London, 
 1854. 
 
 On the supposed fish remains figured' 
 
 on plate 4 of “ The Silurian system. 
 
 In Quart. Jour. Geol. Soc. London, vol. 9, 
 1853, p. 13. 
 
 A synopsis of the classification of 
 
 the British Palaeozoic rocks, by Adam 
 Sedgwick ; with a systematic descrip- 
 tion of the British Palaeozoic fossils in 
 the Geological Museum of Cambridge, 
 by Frederick McCoy, with figures of the 
 new and imperfectly known species. 
 London and Cambridge, 1855, 25 pis. 
 Pt. 2. Palaeontology. 
 
V0GDES.J 
 
 LIST OF AUTHORS. 
 
 49 
 
 McCoy (Frederick) — Continued. 
 
 Fasciculus 1. Radiata and Articulata. Lon- 
 don, 1851. 
 
 Fasciculus 2. Lower and Middle Palaeozoic 
 Mollusca. London, 1852. 
 
 Fasciculus 3. Upper Palaeozoic Mollusca and 
 fish. London and Cambridge, 1855. 
 
 Harpes, Foroesia , Phacops , Odontochile, Ohas- 
 mops, Portlockia, Calymene, Homalonotus , Tro- 
 churus, Lichas, Trinucleus, Harpidella, Tretas -- 
 pis, Ampyx, Isotelus, Ogygia, Barrandia, Ad, 
 daspis, Ceraurus, Eccoptochile, Staurocephalus- 
 Encrinurus, Zethus, Illcenus, Dysplanus, Bi 
 plorhina, Agnostus, Acanthopyge, Eurypterus, 
 Pterygotus, Leptocheles n. g., Ceratiocaris, Bey- 
 richia, Cytheropsis, Trinodus. 
 
 Contributions to British palaeon- 
 tology, or first description of 360 species 
 and several genera of fossil Radiata, 
 Articulata, Mollusca and Pisces from 
 the Tertiary, Cretaceous, Oolitic and 
 Palaeozoic strata of Great Britain. Re- 
 published from the Annals Mag. Nat. 
 Hist. Cambridge, 1854. 
 
 For a list of the genera of fossil Crustacea, 
 see entries under McCoy (Frederick), Annals 
 Mag. Nat. Hist., 2d series, London, vol. 4, 1849. 
 
 Geological Survey of Victoria. Pro- 
 
 dromus of the palaeontology of Vic- 
 toria, or figures and descriptions of 
 Victorian organic remains, decade 3. 
 Melbourne and London, 1875, pis. 22, 23. 
 
 Phacops ( Odontochile ) caudatus , P. ( Port- 
 lockia ) fecundus, Forbesia euryseps McCoy, 
 Licha8 australis McCoy, Homalonotus harri- 
 soni McCoy. 
 
 Mantell ( G. ) Medals of creation, or 
 first lessons in geology and the study 
 of organic remains. 2 vols. London, 
 1854. 
 
 Marcou (Jules). On the Primordial 
 fauna and the Taconic system, by 
 Joachim Barrande ; with additional 
 notes by Jules Marcou. 
 
 In Proc. Boston Soc. Nat. Hist., vol. 7, 1861. 
 p. 369. 
 
 Notice sur les gisements des lentilles 
 
 trilobitif&res taconique de la Pointe 
 LAvis ou Canada. 
 
 In Bull. Soc. G6ol. France, 2d series, vol. 21, 
 
 1864, p. 236. 
 
 Marr (J. E.) On some well-defined life 
 zones in the lower part of the Silurian 
 (Sedgwick) of the Lake District. 
 
 In Quart. Jour. Geol. Soc. London, vol. 34, 
 1878, p. 871. 
 
 Appendix. On some species of Phacops , p. 
 
 884. 
 
 Marr (J. E.) — Continued. 
 
 and Nicholson <H. A.) The Stock- 
 
 dale shales. 
 
 In Quart. Jour. Geol. Soc. London, vol. 44, 
 1888, p. 654, pi. 16. 
 
 Harpes, Proctus, Phacops , Ampyx, Acidaspis, 
 Oheiruru8. 
 
 Martin (D. S.) A new Eurypterid from 
 the Catskiil group. 
 
 In Trans. New York Acad. Sci., vol. 2, 1882, 
 
 p.8. 
 
 This notice was based upon a cast of Sty- 
 lonurus excelsior Hall, obtained from the Mu- 
 seum of Natural History, Albany, New York. 
 Martin (W.) Petrificata Derbiensia: a 
 description of petrifactions collected in 
 Derbyshire. Wigan, 1809, 4to, 53 pis. 
 
 Entomolithue oniscites (derbiensis) , pi. 45, figs. 
 1-3; Entomolithus monoculites ? ( lunatus ), pi. 
 45, fig. 4; Entom. paradoxus, from Dudley, pi. 
 45. fig. 3; also pi. 45a;, fig. 3. 
 
 These fossils have been referred to the fol- 
 lowing modern genera: Phillip sia derbiensis, pi. 
 45, figs. 1-3, and pi. 45a;, fig. 3 ; Belinurus, pi. 
 45, fig. 4, Calymene blumenbachi, pi. 45, fig. 3. 
 
 Matthew (G. F.) Illustrations of the 
 fauna of the St. John group. No. 1. 
 The Paradoxides; their history. 
 
 In Trans. Royal Soc. Canada, vol. 1, 1882, Sec. 
 4, p. 87, pi. 9. 
 
 Paradoxides etemenicus Matt., Par. acadicus 
 Matt., P. lamellatus Hartt. 
 
 Illustrations of the fauna of the St. 
 
 John group. No. 1. The Paradoxides 
 (supplementary section describing the 
 parts). 
 
 In Trans. Royal Soc. Canada, vol. 1, 1882, Sec. 
 4, p. 271, pi. 10. 
 
 Illustrations of the fauna of the St. 
 
 John group, continued: On the Cono- 
 coryphea , with further remarks on Para- 
 doxides. 
 
 In Trans. Royal Soc. Canada, vol. 2, 1884, Sec. 
 4, p. 99, pl.l. 
 
 Paradoxides, Otenocephalus, Oonocoryphe. 
 
 In his explanation of the plate, fig. 6, the au- 
 thor uses a now subgenus, Otenocephalus ( Har - 
 tella) matthewi, and also for fig. 22, Oonocoryphe 
 (Bailiella) baileyi. 
 
 An outline of recent discoveries in 
 
 the St. John group. 
 
 In Bull. New Brunswick Nat. Hist. Soc., No 
 4, 1884. 
 
 Illustrations of the fauna of the St. 
 
 John group. No. 3. Descriptions of 
 new genera and species (including a 
 description of a new species of Soleno- 
 pleura, by J. F. Whiteaves). 
 
 In Trans. Royal Soc. Canada, vol. 3, 1885, p. 29, 
 3 pis. 
 
 BULL. 03 1 
 
A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 50 
 
 Matthew (G.F.)— Continued. 
 
 Lepidittan. g., Lepidillavc. g., Beyrichia, Hip- 
 ponicharion n. g., Beyrichona n. g., Primitia , 
 Agnostics, Hicrodiscus, Agraulos, Solenopleurcc, 
 Paradoxides. 
 
 On the probable occurrence of the 
 
 great Welsh Paradoxides , P. davidis, in 
 America. 
 
 In Am. Jour. Sci., 3d series, vol. 30, 1885, p. 72; 
 Nature, vol. 32, 1885, p. 358. 
 
 Abstract of a paper on the Cambrian 
 
 fauna of Cape Breton and Newfound- 
 land. 
 
 In Canadian Record Sci., vol. 2, 1886, p. 255. 
 
 Note on the occurrence of Olenellus? 
 
 kjerulfi in America. 
 
 In Am. Jour. Sci., 3d series, vol. 31, 1886, p. 472. 
 
 On the Cambrian fauna of Cape Bre- 
 ton and Newfoundland. 
 
 In Trans. Royal Soc. Canada, vol. 2, 1886, p. 
 
 147. 
 
 Agraulos, Selenopleura. 
 
 Illustrations of the fauna of the St. 
 
 John “group. No. 4. On the smaller 
 eyedTrilobites of Division 1, with a few 
 remarks on the species of the higher 
 division of the group. 
 
 In Canadian Record Sci., vol. 2, No. 6, 1887, p. 
 357. 
 
 On the kin of Paradoxides ( Olenellus ?) 
 
 lcjerulji. 
 
 In Am. Jour. Sci., 3d series, vol. 33, 1887, p. 
 390. 
 
 The great Acadian Paradoxides. 
 
 In Am. Jour. Sci., 3d series, vol. 33, 1887, p. 
 388. 
 
 Paradoxides regina Matt. 
 
 Illustrations of the fauna of the St. 
 
 John group. No. 4. Part 1. Descrip- 
 tion of a new species of Paradoxides ( P. 
 regina ). Part 2. The smaller Trilo- 
 bites with eyes ( Ptychoparidce and El- 
 lipsocephalidce ). 
 
 In Trans. Royal Soc. Canada, vol. 5, 1887, p. 
 115, 3 pis. 
 
 Paradoxides, Liostracus, Strenuella n. sub- 
 gen., Ptychoparia, Solenopleurcc, Agraulos, Ellip- 
 socephalus. 
 
 Maurer (F.) Palaontologische Studien 
 im Gebiet des rheinischen Devon. Die 
 Fauna des Rotheisenstein der Grube 
 Haina. 
 
 In Neues Jahrbuch fur Mineral., 1875, p. 596, 
 
 pi. 14. 
 
 Phcccops latifrons, Cypliaspis ceratophtlial- 
 
 mus. 
 
 Maurer (F.)— Continued. 
 
 Palaontologische Studien im Gebiet 
 
 des rheinischen Devon. Die Thon- ' 
 schiefer des Ruppbachthales bei Diez. 
 
 In Neues Jahrbuch fur Mineral., 1876, p. 8&8, 
 pi. 14. 
 
 Phacops, Acidaspis, Brontcus. 
 
 Die Fauna der Kalke von Wald- 
 
 girmes bei Giessen. 
 
 In Abhandl. grossh.-hess. geol. Landesanstalt 
 zu Darmstadt, vol. 1, pt. 2, 1885, atlas of 11 pis. 
 
 Harpes, Phacops, Proetus, Gyphaspis, Oheiru- 
 rus, Bronteus, Primitia, Orozoe. 
 
 Meek (F. B.) Note on Belinurus dance , 
 from the Illinois Coal Measures. 
 
 In Am. Jour. Sci., 2d series, vol. 43, 1867, p. 
 257 ; Geol. Survey Illinois, vol. 2, p. 395. 
 
 Note on a new genus of fossil Crus- 
 tacea. 
 
 In Am. Jour. Sci., 2d series, vol. 43, 1867, p. 
 394 ; Geol. Survey Illinois, vol. 3, p. 547. 
 
 Euproops (n. g.). 
 
 Descriptions of fossils collected by 
 
 the U. S. Geological Survey, under 
 charge of Clarence King. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 22, 1870, 
 p. 56. 
 
 Republished and illustrated in Rept. U. S. 
 Geol. Expl., 40th Parallel, vol. 4, pt. 1, pp. 
 1-197, pis. 1-17. 
 
 Paradoxides , Conocoryphe ( Conocephalites ), 
 Olenics. 
 
 Descriptions of new species of in-. 
 
 vertebrate fossils from the Carbonifer- 
 ous and Devonian rocks of Ohio. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 23, 1§71, 
 p. 57. 
 
 Republished and figured in “ Palseontology 
 of Ohio,” vol. 1, 1873, p. 233, 23 pis. 
 
 Proetus planimarginatus, Dalmanites ohio- 
 ensis. 
 
 Descriptions of new Western Palaeo- , 
 
 zoic fossils, mainly from the Cincin- 
 nati group of the Lower Silurian seriea 
 of Ohio. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 23, 1871, p* 
 308. 
 
 Redescribed and illustrated in “Palaeontol- 
 ogy of Ohio,” vol. 2, 1875. 
 
 Gythere, Ceratiocaris ( Colpocaris ), Archceoca- 
 ris, Solenocaris, Colpocaris. (Not Solenocarie 
 Young, 1868.) 
 
 List of Carboniferous fossils from 
 
 West Virginia, with descriptions of 
 new species. 
 
 In Appendix B, Rept. of Regents of West 
 Virginia Univ., 1870, Wheeling, 1871, p. 68. 
 
 Phillipsia stevensoni Meek. 
 
 Final report of the U. S. Geological, 
 
 Survey of Nebraska and portions of the 
 
VOGDES.] 
 
 LIST OF AUTHORS. 51 
 
 Meek (F. B.)— Continued, 
 adjacent Territories, by F. V. Hayden, 
 etc. Report on the paleontology of 
 eastern Nebraska, with some remarks 
 on the Carboniferous rock of that 
 district by F. B. Meek. Washington, 
 1871, p. 83, 11 pis. ( Two editions : 
 first in 8vo, second in 4to.) 
 
 Phillipsia, Gythere. 
 
 Genus Archceocaris. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 24, 1872, 
 p. 325. 
 
 Description of new species of fossils 
 
 from Cincinnati group, Ohio. 
 
 In Am. Jour. Sci., 3d series, vol. 3, 1873, p. 423. 
 
 Proetus, Dalmanites. 
 
 Preliminary palaeontological report, 
 
 consisting of list and descriptions of 
 fossils, with remarks on the age of tbe 
 rocks in which they are found, etc. 
 
 In Sixth Ann. Kept. U. S. Geol. Survey Terri- 
 tories, embracing portions of Montana, Idaho, 
 "Wyoming, and Utah, etc. F. V. Hayden, 
 Washington, 1873, p.431. 
 
 Conocoryphe (Ptychoparia) , Bathyurus, Ba- 
 
 „ thyurella (Asaphiscus) n. sg., Asaphus, (Megal- 
 aspis), Agnostus. 
 
 Report of the Geological Survey of 
 
 Ohio. Vol. 1. Geology and palaeon- 
 tology. Pt.2. Palaeontology. Descrip- 
 tions of invertebrate fossils of the Silu- 
 rian and Devonian systems, by F. B. 
 Meek. 
 
 Columbus, 1873. pp. 1-243, pis. 1-23. 
 
 Proetus, Dalmanites , Calymene, Asajjhus 
 ( Dotelus ), Acidaspis, Ceraurus, Illcenus (Bu- 
 mastu8), Gythere , Leperditia. 
 
 Descriptions of Olenus ( Olenellus ) 
 
 gilberti and Olenus (Olenellus) hoivelli. 
 
 In Kept. Geog. and Geol. Expl. Surveys West 
 100th Her., vol. 3, Washington, 1875, p. 182. 
 
 A report on some of the invertebrate 
 
 fossils of the Waverly group and Coal 
 Measures of Ohio. 
 
 In Kept. Geol. Survey Ohio. Vol. 2. Geology 
 and Palaeontology. Pt. 2. 1875, pp. 269-347, pis. 
 10 - 20 . 
 
 Phillipsia , Griffithides, Geratiocaris ( Oolpo - 
 caris), Geratiocaris ( Solenocaris ), Archceocaris , 
 
 Oolpocaris, Solenocaris. 
 
 Palaeontology. 
 
 In U. S. Geol. Expl. 40th Parallel, vol. 4, pt. 1, 
 1877, pp. 1-197, pis. 1-17. 
 
 Paradoxules , Gonocoryphe ( Ptychoparia ), 
 Proetus, Dalmanites. 
 
 and Hayden (F. V.) Descriptions 
 
 of new Lower Silurian, Jurassic, Creta- 
 ceous, aud Tertiary fossils collected in 
 
 Meek (F. B.) and Hayden (F. V.)— Con- 
 tinued. 
 
 Nebraska by the exploring expedition 
 under the command of Capt. W. F. 
 Raynolds, U. S. Top. Eng., with re- 
 marks on the rocks from which they 
 were obtained. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 13, 1862, 
 p. 415. 
 
 Arionellus, Arionellus ( Grepicephalus ) oweni. 
 
 Palaeontology of the Upper Mis- 
 souri. A report upon collections made 
 principally by the expeditious under 
 command of Lieut. G. K. Warren, U. S. 
 Top. Eng., in 1855-56. Invertebrates. 
 Pt. 1. 
 
 In Smithsonian Contrib., No. 172, Washing- 
 ton, 1864, 5 pis. 
 
 Paradoxides, Agraulos , Agraulos oweni M. 
 & H. 
 
 and Worthen (A. H.) Notice of 
 
 some new types of organic remains from 
 the Coal Measures of Illinois. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 17, 1865, 
 p. 41. 
 
 Acanthotelson n. g., Belinurus , Anthrapalce- 
 mon, Palceocaris n. g. 
 
 Contributions to the palaeou- 
 
 - tology of Illinois and other Western 
 States. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 17, 1865, 
 p. 245. 
 
 Proetus, Phillipsia, Griffithides, Dalmania, 
 Lichas. 
 
 Descriptions of invertebrates 
 
 from the Carboniferous system. 
 
 In Geol. Survey Illinois, vol. 2, 1866, p. 145, pis. 
 14-20, 23-32. 
 
 Belinurus, Acanthotelson , Palceocaris, An- 
 thrapalcemon. 
 
 — — Preliminary notice of a scor- 
 pion, a Eurypterus, and other fossils 
 from the Coal Measures of Illinois. 
 
 In Am. Jour. Sci., 2d series, vol. 46, 1868, p. 19. 
 Republished and illustrated in “Geol. Survey 
 Illinois,” vol. 3, p. 560. 
 
 Palaeontology. 
 
 In Geol. Survey Illinois, vol. 3, 1868, pp. 291- 
 565, pis. 1-20. 
 
 Proetus, Phacops, Dalmanites ( Odonocepha - 
 lus), Lichas, Acidaspis, Illcenus, Ceratiocaris, 
 Euproops , Palceocaris, Euryplerus (Anthrapa- 
 Icemon), Acanthotelson. 
 
 Descriptions of a now species 
 
 and genera of fossils from tlio Palaeo- 
 zoic rocks of the Western States. 
 
 In Proc. Acad. Nat. Sci. Phila., 2d series, vol. 
 
 | 14, 1870, p. 22. 
 
52 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 
 [BULL. 63. 
 
 Meek (F. B.) and Wortfcen (A. H.)— 
 Continued. 
 
 Phillip si a tuberculata M. & W., Phillipsia 
 (Griffithides) bufo M. & W., Asaphus (Isotelus) 
 vigilant M. & W., Ulcenus ( Bumastus ) graf- 
 tonensis M. & "W., Dithyrocaris carbonarius 
 M.& W. 
 
 Descriptions of invertebrates 
 
 from tbe Carboniferous system. 
 
 In Geol. Survey Illinois, vol. 5, 1873, pp. 323- 
 619, pis. 1-32. 
 
 Phillipsia ( Griffithides ) portlocki, Phillipsia 
 ( Griffithides ) bufo, Phillipsia (Griffithides) sci- 
 tula, Dithyocari8 carbonarius. 
 
 Description of tbe inverte- 
 brates. 
 
 In Geol. Survey Illinois, vol. 6, 1875, pp. 489- 
 532, pis. 23-33. 
 
 Lichas, Asaphus (Isotelus), Sphcerexochus, 
 Ulcenus (Bumastus). 
 
 Meneghini (Giuseppe). Nuovi fossiii si- 
 luriani di Sardegna. 
 
 In Atti reale Accad. Lincei, Roma, 1880, 1 pi. 
 
 Dalmanites, Lamarmorce. 
 
 Posizione relativa dei varii piani 
 
 siluriani dell’ Iglesiente in Sardegna. 
 
 In Pfoc. verb. Soc. Toscana Sci. Nat., 1881, p. 
 258. 
 
 Paradoxides, Trinucleus , Dalmanites , Conoce- 
 phalites. 
 
 Fauna Cambriana dell’ Iglesiente in 
 
 Sardegna. 
 
 In Proc. verb. Soc. Toscana Sci. Nat., 1881, p. 
 158. 
 
 Paradoxides, Olenus, Conocephalites. 
 
 Nuovi Trilobiti di Sardegna. 
 
 In Proc. verb. Soc. Toscana Sci. Nat., 1881, p. 
 
 200 . 
 
 Paradoxides, Conocephalites. 
 
 Note alia fauna Cambriana dell’ 
 
 Iglesiente. 
 
 In Proc. verb. Soc. Toscana Sci. Nat., 1882, 
 p.7. 
 
 Olenus, Anomocare, Conocephalites, Platypel m 
 tis. 
 
 Nuovi fossiii Cambrian i di Sardegna. 
 
 In Proc. verb. Soc. Toscana Sci. Nat., 1884, 
 p. 56. 
 
 Conocephalites, Anomocare. 
 
 Palaeontologia dell’ Iglesiente in 
 
 Sardegna. Fauna Cambriana trilo- 
 biti. 
 
 In Mem. R. Com. Geol. Italia, vol. 3, 1888, pt. 
 2, 49 pp., 7 pis. 
 
 Paradoxides, Olenus, Anomocare, Conocepha m 
 lites, Asaphus (Platypeltis), Conocoryphc. 
 
 Meyer (H. von). Beitriige zur Petre- 
 facten-Kunde. 
 
 In Nova Acta Acad. Leop. Carol., vol. 15, 1831, 
 p. 57, pi. 56, fig. 13. See, also, Neues Jabrbuch 
 fur Mineral., 1833, p. 481. 
 
 Calymene cequalis Meyer. 
 
 Meyer (H. von) and Munster (G. G. zu). 
 Beitrage zur Petrefacten-Kunde. Bay- 
 reuth, 1840., pt. 3, pi. 5. 
 
 Calymene variolaris, C. intermedia, C. Icevis, 
 
 C. sternbergi, C. propinqua, O. articulata , Asa- 
 phus? caudori, A. pusillus, A.? brevis, A. 
 grandis, Ulcenus perovalisf, Paradoxides brevi- . 
 mucronatus, Brontes radiatus, B. costatus, B. 
 subradiatus, Bumastus Jr ankonicus, B. planus, 
 Harpes speciosus, Trinucleus gracilis, T.tvil- 
 kensii, T. ellipticus, T. nelsoni, T. ? otarion, T. ? 
 gibbosus, Agnostus pisiformis. 
 
 Beitrage zu Petrefacten-Kunde. 
 
 Bayreuth, 1842, pt. 5, p. 112. Nachtrag 
 zu den Yersteinerungen des Ueber- ' 
 gangs-Kalkes mit Clymenien von Ober- 
 franken vom Herausgeber. 
 
 Calymene marginata, pi. 10, fig. 6 ; C.furcata, 
 Asaphus dubius, Ellipsocephalus hoffi, Otarion ' 
 elegans, Harpes, Trinucleus? Icevis, T. inter me- 
 dius, T. nilsoni. 
 
 Squaliden-Reste aus dem Posidono- 
 
 myen-Schiefer des Oberharzes bei Ober- 
 Schulenburg. 
 
 In Danker and von Meyer “ Palaeont., ” vol. 
 
 3, Cassel, 1854, p. 53. 
 
 Harpes, Proetus, Phacops, Lichas, Cheirurus. 
 
 See, also, Jordon (H.) and Meyer (H. von). - \ 
 
 Mickleborough ( John ). Locomotory 
 appendages of Trilobites. 
 
 In Jour. Cincinnati Soc. Nat. Hist., vol. 6, 1883, 
 p. 200, figs. 1-3. Noticed: Am. Jour. Sci., 3d 
 series, vol. 27, 1884, p.409; Geol. Mag., n. s., de- 
 cade 3, vol. 1, London, 1884, p. 80. 
 
 Asaphus megistos Locke. 
 
 Miller (S. A ) Monograph of the Crusta- 
 cea of the Cincinnati group. 
 
 In Cincinnati Quart. Jour. Sci., vol. 1, 1874, p. 
 115. 
 
 Triarthrus, Proetus, Dalmanites, Calymene^ 
 Lichas, Trinucleus, Asaphus, Isotelus, Acid- 
 aspis, Ceraurus, Beyrichia, Leper ditia, Cy there.' 
 
 The author, in his classification aud generic 
 descriptions, has generally followed McCoy 
 (“Brit. Palaeozoic Bocks,” 1855). He gives a 
 description of the different fossil Crustacea oc- 
 curring in the Cincinnati group, and figures 
 Leperditia byrnesi Miller, and a wood-cut rep- 
 resenting the tracks of an Asaphus (?). 
 
 [No title. — Description of new spe- 
 cies of Palaeozoic Entomostraca.] 
 
 In Cincinnati Quart. Jour. Sci., vol. 1, 1874, p. 
 
 232. 
 
 Beyrichia duryi, B. striato-marginatus, B. 
 chambersi. 
 
 Some new species of fossils from the 
 
 Cincinnati group, and remarks upon 
 some described forms. 
 
 In Cincinnati Quart. Jour. Sci., vqI, 2, 1875, 
 p. 349, figures. 
 
 Acidaspis, Beyrichia, Leperditia. 
 
vOgdes.] 
 
 LIST OF AUTHORS. 
 
 53 
 
 Miller (S. A. )— Continued. 
 
 The American Palaeozoic fossils. A 
 
 catalogue of the genera and species, 
 with names of authors, dates, places of 
 publication, group of rocks in which 
 found, and the etymology and significa- 
 tion of the words, etc. Cincinnati, 
 1877. Also a 2d ed., with supplement. 
 
 Description of a new genus and 
 
 eleven new species of fossils, with re- 
 marks upon others well known, from 
 the Cincinnati group. 
 
 In Jour. Cincinnati Soc. Hat. Hist., vol. 1, 
 1878-79, p. 100, pi. 3. 
 
 Lichas harrisi, Cythcre irregularis. 
 
 Description of two new species from 
 
 the Niagara group, and five from the 
 Keokuk group. 
 
 In Jour. Cincinnati Soc. Hat. Hist., vol. 2, 
 1879, p. 254, pi. 15. 
 
 Encrinurus egani. 
 
 Description of new species of fossils. 
 
 In Jour. Cincinnati Soc. Hat. Hist., vol. 4, 
 
 1881, p. 259, pi. G. 
 
 Leperditia coecigena. 
 
 Description of three new species, 
 
 and remarks upon others. 
 
 In Jour. Cincinnati Soc. Hat. Hist., vol. 5, 
 
 1882, p. 116, pi. 5. 
 
 Calymene callicephala Green. 
 
 Milne-Edwards (H.) Sur les affinitds 
 des Trilobites. 
 
 In Institut de France, Acad. Royale Sci., 
 vol. 1, 1827, p. 254. 
 
 Trilobites dans Lamarck's “Histoire 
 
 natnrelle des animaux sans vertkbres.” 
 Vol. 5. Paris, 1838, p. 220. 
 
 Paradoxides, Ellipsocephalus, Conocephalus , 
 Triarthrus , Calymene , Ampyx, Asaphus, Ogygia, 
 Otarion, Agnostus, Ceraurus, Oypridina n. g. 
 
 Histoire naturelle des Crustac^s, 
 
 comprenant l'anatomie, la physiologie 
 et la classification de ces animaux. 
 [3 vols., with atlas of plates.] Paris, 
 1834-’40. 
 
 The Trilobites are described in vol. 3, pp. 
 285-346, in the following order: Nileus, Am- 
 pyx, Isotelus, Asaphus , Ilomalonotus, Calymene, 
 Pleuracanthe n. g. (referred by author to Dal- 
 manites), Trinucleus, Otarion, Ogygia, Para- 
 doxides, Peltura n. g. (the first species cited 
 by the author under this new genus was: 
 Peltura scaraboeoides Wablenburg; the second, 
 Peltura bucklandi Milne-Edwards, is a species 
 of the genus Lichas), Agnostus, Eurypterus. 
 Classifies 64 species under 13 genera. 
 
 ■ Report on the palaeontological re- 
 
 searches of M. Marie Ronault in Brit- 
 tany and Anjou. 
 
 Milne-Edwards (H.) — Continued. 
 
 In Coraptes Rendus Acad. Sci. Paris, 1847, vol. 
 24, p. 593; Bull. Soc. G6ol. France, vol. 4, 1847, 
 p. 309; Quart. Jour. Geol. Soc. London, vol. 4, 
 1848, pt. 2, Miscellaneous, p. 35. 
 
 Trimccleus, Calymene, Phacops , Polyeres n. 
 g., Prionocheilus, Cheirurus, Nileus, Ogygia, 
 I llcenus. 
 
 Structure des Trilobites. 
 
 In Annales Sci. Hat., vol. 12, 1881, 33 pp., pis. 
 1-3. 
 
 A review of C. D. Walcott’s “Organization 
 of Trilobites.” 
 
 Acidaspis, Calymene, Ceraurus, Trinucleus, 
 Asaphus, Eurypterus. 
 
 Mitchell (John). On some new Trilo- 
 bites from Bowning, N. S. W. 
 
 In Proc. Linnean Soc. Hew South Wales, 2d 
 series, vol. 2, 1887, p. 435, pi. 16. 
 
 Proetus bowningensis, Cyphaspis bownin- 
 gensis, Bronteus longispinifer. 
 
 On a new Trilobite from Bcwning. 
 
 In Proc. Linnean Soc. Hew South Wales, 2d 
 series, vol. 3, 1888, p. 397, pi. 16 of vol. 2. 
 
 Acidaspis longispinis. 
 
 Mitchell (Samuel L.) An account of the 
 impressions of a fish in the rocks of 
 Oneida County, New York. 
 
 In Am. Monthly Mag., vol. 3, 1818, p. 291. 
 
 The author states that the Hew York fossil, 
 from the town of Westmoreland, “is separated 
 into plates, like those of an insect or crusta- 
 ceous animal, reaching from side to side quite 
 across the back. Eleven entire plates and part 
 of the twelfth can be counted. They are not so 
 broad near the head and thorax as they are on 
 approaching the tail ; for between the pectoral 
 fins they fall short of a quarter of an inch, 
 while on approaching the caudal fin they grad- 
 ually enlarge until they exceed that measure.” 
 
 Eurypterus remipes De Kay. 
 
 Modeer (A.) Anmerkungen fiber einige 
 nerikische Versteiner ungen. (*) 
 
 In Berlin. Gesell. naturf. Freunde, vol. 6, 
 1785, p. 247, pi. 2, figs. 1-8-12. 
 
 (Agnostus pisiformis), pi. 2, figs. 1 , 2 ; (Olenus 
 gibbosus), pi. 2, figs. 3-5; (Olenus scaraboeoides), 
 pl. 2, fig. 7. 
 
 Moller (Valerian von). Ueber die Trilo- 
 biteu der Steinkohlenformation des 
 Ural, nebst einer Uebersicht und eini- 
 gen Ergiinzungen der bisherigen Beob- 
 achtuugen fiber Kohlen-Trilobiten im 
 Allgemeinen. Moscou, 1867. 1 pl. 
 
 In Bull. Soc. Imp. des Haturalistes Moscou, 
 Ho. 1, 1867. 
 
 Qrijjlthides, Phillipsia , Brachymetopus. 
 
 Morris ( J. ) Catalogue of British fossils. 
 London, 1843. 2d ed., London, 1854. 
 
54 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull.. 63. 
 
 Mortimer (C.) The description and fig- 
 ures of a small, flat, spheroidal stone 
 having lines formed on it. 
 
 In Philos. Trans. Royal Soc. London, voL 
 46, 1760, p. 602, pis. 1, 2. 
 
 ( Calymene blumenbachi.) 
 
 Miiller (O. F.) Entomostraca sen insecta 
 testacea quse in aquis Daniae et Nor- 
 wegiae reperit, etc. Lipsiae et Hafniae, 
 1785. 21 pis. 
 
 Cythere n. g. 
 
 The generic term Cytherina was substituted 
 by Lamarck for Muller’s Cythere, and has been 
 used by many authors. Prof. J. D. Dana uses 
 the term Cytherina to represent a subgenus. 
 
 Munster (G. G.) Ueber einige fossile 
 Arten Cypris und Cythere. 
 
 In Jahrbuch fur Mineral., 1830, p. 60. 
 
 Cythere hissingeri. 
 
 and Meyer (H. von). See Meyer 
 
 and Miinster. 
 
 Murchison (R. I.) The Silurian system, 
 founded on geological researches in 
 the counties of Salop, Hereford, Rad- 
 nor, q^fcc. [London, 2 vols., 1839, 40 
 pis., and 3 larg c maps in folio.] 
 
 Calymene, Homalonotus, Asaphus, Ogygia, 
 Illcenus, JBumastus n. g., Acidaspis n. g., Trinu- 
 cleus n. g., Agnostus. 
 
 Metamorphosis of certain Trilobites 
 
 as recently discovered by M. Barrande. 
 
 In Rept. 19th Meeting Brit. Assoc. Adv. 
 Sci., 1849, Trans. Sec., p. 58. 
 
 On the Silurian rocks of the south 
 
 ot Scotland, with a list and descrip- 
 tion of the Silurian fossils of Ayrshire, 
 by J. W. Salter. 
 
 In Quart. Jour. Geol. Soc. London, vol. 7, 
 1851, p. 137, pis. 8-10. 
 
 Cheirurus gelasinosus Port., Asaphus sp. 1, 
 Calymene blumenbachi Brong., Phacops stokesii 
 Milne -Edwards, Illcenus bowmani? , Lichas 
 laxatus McCoy, Encrinurus punctatus Briin. 
 
 Siluria. A history of the oldest 
 
 rocks in the British Isles and other 
 countries. [London, 1854, geol. map, 
 37 pis. 3d ed., London, 1859, geol. 
 map, 41 pis. 4th ed., London, 1867, 
 geol. map, 42 pis.] 
 
 The figures are all transferred from the 
 original plates in the “Silurian system.” In 
 every case where the old name has been 
 changed, in accordance with more recent no- 
 menclature, the name used in the original 
 work is inserted in brackets. 
 
 , Verneuil (E. de) and Keyserling 
 
 (Alex. von). Geology and palaeontol- 
 ogy of Russia and the Ural Mountains. 
 
 Murchison (R. I.) and Verneuil (E. de) — 
 Continued. 
 
 [London, 1845, 2 vols., 50 pis. Palae- 
 ontology, vol. 2; Crustacea, p. 376, 
 pi. 27.] 
 
 Asaphus expansas Dalm., Phillipsia eich- 
 waldi Fischer, P. ouradica n. s., Calymene- 
 odeni Eichw., O. fischeri Eichw. 
 
 Nathorst (A. G. ) Om lager-foljden inom 
 i Cambriska formationen vid Andrarum 
 I i Skane. 
 
 In Ofversigt kongl. Svenska Vet.-Akad. For- 
 handl., 1869, No. 1, p. 61. 
 
 Om de Kambriska och Siluriska la- 
 
 gren vid Kiviksesperid i Skane jeuite 
 anmarkningar om primordial faunans 
 lager vid Andrarum. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 No. 37, vol. 3, 1876. 
 
 Om det inbordes forhallandet af la- 
 
 gren med Paradoxides olandicud och P. _ 
 tessini pa Oland. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 No. 69, vol. 5, 1881. 
 
 Om det iubordes aldersforhallandet 
 
 mellan zonerna med Olenellus kjerulfi 
 och Paradoxides olandicus. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 No. 71, vol. 6, 1882. 
 
 The position of the Olenellus beds. 
 
 In Am. Geol., vol. 2, 1888, p. 356. 
 
 Newberry (J. S.) China, by Ferdinand 
 F. von Richthofen. Vol. 4. Berlin, I 
 1883. * 
 
 In Am. Jour. Sci., 3d series, vol. 26, 1883, p. 
 152. 
 
 This is a notice of the palaeontological vol- 
 ume. 
 
 Nicholson (H. A.) A manual of palaeon- I 
 tology for the use of students, with a : 
 general introduction on the principles 9 
 of palseon tology, in two volumes. Vol. | 
 1. Edinburgh and London, 1879. Cru- I 
 stacea, Chapter xvm. 
 
 Harpes, Remopleurides, Paradoxides, Anopo - | 
 lenus, Dicellocephalus, Hydrocephalus, Olenua, I 
 Parabolina, Triarthrus, Bohemilla, Conocepha -' I 
 lites, Angelina, Ellipsocephalus, Sao, Proetua, j 
 Arethusina, Phillipsia, GriJJithides, Bathymeto- I 
 pus, Phacops, Dalmanites, Calymene, Homalo- I 
 notus, Lichas, Trinucleus, Ampyx, Dionide, I 
 JEglina, Asaphus, Ogygia, Barrandia, Niobe, I 
 N ileus, Stygina, Illcenus, Acidaspis , Cheirurus, I 
 Sphcerexochus, Areia, Placoparia, Cromus, En- j 
 crinurus, Cybcle, Dindymcne, Bronteus, Agnoa- I 
 tus, Microdiscus, Protichnites, Ai’istozoe, Beyri- I 
 chia, Leperditia, Primitia, Entomis, Cythere , I 
 Eurypterus, Pterygotus, Isochilina, Cypris, I 
 Candona, Orozoe, Callizoe, Kirkbya, Moorea, R 
 Cryprulina, Cytherella, Cytherellina, AZchmina, H 
 
 H 
 
VOGDK6.J 
 
 LIST OF AUTHORS. 
 
 55 
 
 Nicholson (H. A.) Continued. 
 
 Bairdia, Hymenocaris, Caryocaris, Peltocaris, 
 Pisdnocaris, Aptychopis, Pterocaris , Gryptoca- 
 ris, Ceratiocaris, Pithyrocaris, Aspidocaris, Es- 
 theria, Psilocephalus , Hemiaspis, Exapinurus , 
 Pseudoniscus, Stylonurus , Neolimulus, Prestwi- 
 chia , Belinurus. 
 
 and Etheridge, jr. (R.) A mono- 
 graph of the Silurian fossils of the Gi- 
 van District, in Ayeshire, etc. Vol. 1, 
 1878-’80, 24 pis. 
 
 Fasciculus I. Rhizopoda, Actinozoa, and 
 Trilobites (1878). 
 
 Phacops, Calymene, Lichas , Pindymene, 
 Asaphus, Ogygia , Acidaspis, Gheirurus, Sphce- 
 rexochus, Encrinurus , Cybele , Zethus, Atracto- 
 
 pyge- 
 
 Fasciculus II. Trilobita, Phyllopoda, Cir- 
 ripedia, and Oslracoda (1879). 
 
 Bemopleu rides ( Gaphyra ), Proetus, Cyphas- 
 pis, Phacops , Calymene, Lichas, Trinucleus , 
 Ampyx, Salteria, Asaphus, Illoenus, Gheirurus, 
 Acidaspis, Encrinurus, Cybele, Bronteus , Ag- 
 nostus, Bronteopsis, Lonchodomus, Raphiopho- 
 nes, Solenocaris, Pinnocaris Peltocaris, Piety o- 
 caris, Turrilepas, Beyrichia, Primitia, Gythere, 
 Entomis. 
 
 Fasciculus III. The Annelida and Echino- 
 dermata, with supplements on the Protozoa, 
 Coelenterata, and Crustacea (1880). 
 
 Trinucleus, Pionide, Cyclopyge, Staurocepha- 
 lus, Agnostus , Turrilepas. 
 
 Nieszkowski (J.) Der Eurypterus remi- 
 pes aus den ober-silurischen Schichten 
 der Insel Oesel. 
 
 In ArchivNaturk. Liv-, Ehst- u. Kurl., vol. 2, 
 
 1858, p. 299, 2 pis. 
 
 VersoCh einer Monographie der in 
 
 den silurischen Schichten der Ostsee- 
 provinzen vorkommenden Trilobiten. 
 
 In ArcbivNaturk. Liv-, Ehst- u. Kurl., vol. 1, 
 1857, p. 517, 3 pis. 
 
 Proetus, Cyphaspis, Phacops, Calymene, Li- 
 chas, Asaphus, Illoenus, Gheirurus, Sphcerexo- 
 chus, Amphion, Encrinurus, Zethus, Bronteus, 
 
 Platymetopus. 
 
 Zusatze zur Monographie der Trilo- 
 biten der Ostseeprovinzen, nebst der 
 Beschreibung einiger neuen ober- silu- 
 rischen Crustaceen. 
 
 In ArchivKaturk. Liv-, Ebst u. Kurl., vol. 1, 
 
 1859, p. 345, 2 pis. 
 
 Cyphaspis, Lichas, Asaphus, Gheirurus, Sphce - 
 rexochus, Encrinurus, Bronteus, Bunodes, Exa~ 
 pinurus n. g., Pseudoniscus n. g. 
 
 Novak (Ottomar). Studien an Hyposto- 
 men bdhmischer Trilobiten. No. 1. 
 
 In Sitzungsberichte k. bohm.Gesell. Wiss., 
 
 Jahrg. 1879, p. 475. 
 
 Novak (Ottomar) — Continued. 
 
 Harpes, Paraaoxides, Oonocephalites, Proetus, 
 Palmanites, Trinucleus, Ampyx, Acidaspis, 
 Gheirurus, Placoparia, Bronteus, Garmon, 
 Harpina n. g., Galymene, Illoenus, Phacops. 
 
 Studien an Hypostomen bohmischer 
 
 Trilobiten. No. 2. 
 
 In Sitzungsberichte k. bohm. Gesell. Wiss., 
 Jahrg. 1884, 1 pi. 
 
 ILarpes, Harpina, Asaphus, Ogygia , Niobe. 
 
 Zur Kenntniss der bohmischen Trilo- 
 biten. 
 
 In Beitrage zur Palaeontolographie von 
 Oesterrich, Wien, 1884, 5 pis. 
 
 Harpes, Remopleurides , Phillipsia, Dalmani- 
 tes, Galymene, Homalonotus, JEglina, Trinu- 
 cleus, Ampyx, Pionide, Asaphus, Barrandia, 
 Ptychocheilus, Illoenus, Acidaspis, Gheirurus , 
 Placoparia, Cromus , Bronteus, Agnostus. 
 
 Studien an Hypostomen bohmischer 
 
 Trilobiten. No. 3. 
 
 In Sitzungsberichte k. bohm. Gesell. Wiss., 
 Jahrg. 1885, p. 581, 1 pi. 
 
 Phillipsia, Phillip sinella n. g. 
 
 Remarques sur le genre Aristozoe 
 
 Barrande. 
 
 In Sitzungsberichte k. bohm.Gesell. Wiss., 
 Jahrg. 1885, p. 239, 1 pi. 
 
 Aristozoe, Oallizoe, Ceratiocaris, Orozoe. 
 
 Nouveau Crustac6 phyllocaride de 
 
 F6tage F-f 2 en Boheme. 
 
 In Sitzungsberichte k. bohm. Gesell. Wiss., 
 Jahrg. 1885, p. 343, 1 pi. 
 
 Ptychocaris n. g. 
 
 Studien an Hypostomen bohmischer 
 
 Trilobiten. No. 4. 
 
 In Sitzungsberichte k. bohm. Gesell. Wiss., 
 Jahrg. 1886, p. 429, plate. 
 
 Encrinurus, Cromus. 
 
 Zur Kenntniss der Fauna der Rtage 
 
 F-fi in der paheozoischen Schichten- 
 gruppe Bohmens. 
 
 In Sitzungsberichte k. bohm. Gesell. Wiss., 
 Jahrg. 1886, p. 660, 2 pis. 
 
 Aristozoe. 
 
 Note sur Phasganocaris, nouvoau 
 
 Phyllocaride de P6tage F-f 2 en Bo- 
 h§rae. 
 
 In Sitzungsberichte k. bohm. Gesell. Wiss., 
 Jabrg. 1886, p. 498, 1 pi. 
 
 Phasganocaris n. g. 
 
 Oehlert (D.) Sur lea fossiles d6voniens 
 du ddpartement de la Mayeune. 
 
 In Bull. Soc. G6ol. France, 3d series, vol. 5, 
 1877, p. 578, pi. 9. 
 
 Gryphceus michelini, C. jonesi. G. munieri, 
 Homalonotus gervillei, Leperditia britannica, 
 Primitia fischeri. 
 
56 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA, 
 
 [BUIjL. 63. 
 
 Oehlert (D.) Sur le D6vonien du d6- 
 partement de la Sartlie. 
 
 In Bull. Soc. G6ol. France, 3d series, vol. 7, 
 1879, p. 697, pi. 13. 
 
 Proetus guerangeri , Bronteus verneuili. 
 
 Description de Goldins gerville Bar- 
 
 rande. 
 
 In Bull. Soc. d’E tudes Sei., Angers, 1885, 1 pi. 
 
 Etudes sur quelques Trilobites du 
 
 groupe des Proetidse. 
 
 In Bull. Soc. d’Etudes Sci., Angers, 1885, 2 pis. 
 
 The author divides the Proetidae into two 
 divisions on the form of the glabella. 
 
 Sec. A. Glabella conic, genera Proetus, Phce- 
 ton, Dechenella, and Brachymetopus. 
 
 Sec. B. Glabella pyriform, genera Phillip - 
 sella, Phillip sia, and Griffithides. 
 
 Harpes, Gonocephalites, Gyphaspis, Arethu- 
 sina, Galymene, Asaphus, Ogygia, Bronteus. 
 
 Etudes sur quelques fossiles d6vo- 
 
 niens de l’ouest de la France. 
 
 In Bibliotheque de l’Eeole des Hautes 
 Etudes, Sec. Sci. Nat., vol. 33, 1887, 5 pis. 
 
 Proetus oehlerti Bayle, Phacops portieri 
 Bayle. 
 
 Oldham ( 4 T.) On Griffithides glohiceps. 
 
 In Jour. Geol. Soc. Dublin, vol. 3, pt. 3, 1846, 
 p. 188, pi. 2. 
 
 Redrawn, pi. 6, fig. la, b, Woodward’s “Mono, 
 graph British Carboniferous Trilobites,” Lon- 
 don, 1883. 
 
 Ordway (Albert). On the supposed 
 identity of Paradoxides harlani Green 
 with P. spino8us Boeck. 
 
 In Proc. Boston Soc. Nat. Hist., vol. 8, 1861, 
 p. 1, 2 figs. 
 
 The organization of the Trilobites. 
 
 In Geol. Nat. Hist. Repertory, vol. 1, 1865, p. 
 
 12 . 
 
 Owen (D. D.) Report of a geological ex- 
 ploration of part of Iowa, Wisconsin, 
 and Illinois, made under instructions 
 from the Secretary of the Treasury of 
 the United States, in the autumn of the 
 year 1839. Washington, 1840. 
 
 In 26th Cong., H. of Rep., Doc. 239, 2d ed., 
 1844; 28th Cong., Sen. Doc. 407, 18 pis. of 
 fossils. 
 
 PI. 12, fig. 3, Galymene bufo; pi. 16, fig. 1, 
 llloenus trentonensis? (referred by Dr. D. D. 
 Owen, in 1852, to llloenus ovalis); pi. 17, fig. 9, 
 Thaleops?; pi. 18, fig. 2, Asaphus,- pi. 18, fig. 10 
 (Asaphus platycephalus) -, pi. 18, fig. 2, Asaphus. 
 
 Report of a geological reconuois- 
 
 sance of the Chippewa Land District of 
 Wisconsin and incidentally of a portion 
 of the Kickapoo country, and a part of 
 Iowa and of the Minnesota territory, 
 etc. Washington, 1848. 
 
 Owen (D. D.) — Continued. 
 
 This report contains figures of the following 
 fossils, which were afterwar s described by 
 Dr. D. D. Owen under the names of Dikelo- 
 cephalus minnesotensis, pi. 7 .figs. 2, 3 ; Loncho- 
 cephalus hamulus, pi. 7, fig. 5; Dikelo cephalus 
 iowensis, pi. 7, fig. 1. 
 
 Report of a geological survey of Wis- 
 consin, Iowa, and Minnesota, and, inci- 
 dentally, a portion of Nebraska Terri- 
 tory. Philadelphia, 1852, 638 pp., 27 
 pis., 16 sections and maps. 
 
 Dikelocephalus n. g., Loncho cephalus n. g. t 
 Grepicephalus n. g., Menocephalus n. g., Asa- 
 phus ( Isotelus) iowensis. 
 
 Owen (Richard). Description of the im- 
 pressions and foot-prints of the Protich- 
 nites from the Potsdam sandstone of 
 Canada. 
 
 In Quart. Jour. Geol. Soc. London, voL 8, 1852, 
 p. 214, pis. 9-14a. 
 
 Palaeontology, or a systematic sum- 
 mary of extinct animals and their 
 geological relation. Edinburgh, 1861. 
 
 Class 3. Crustacea, pp. 45-51. 
 
 Facht (R.) Geognostische Untersuchun- 
 gen zwischen Orel Woronasch und Sim- 
 birsk im Jahre 1853. 
 
 In Beitrage zur Kenntniss des russischen 
 Reiches und der angranzenden Lander Asiens, 
 St. Petersburg, 1858. 
 
 Packard, jr. (A. S.) On the embryology 
 of Limulus polyphemus. 
 
 In Proc. Am. Assoc. Adv. Sci., 1870, 19th 
 meeting, p. 247. 
 
 Notes on the larva of Trilobites, etc. 
 
 The structure of the eye of Trilo- 
 bites. 
 
 In Am. Naturalist, vol. 14, 1880, p. 503. 
 
 A monograph of the Phyllopod Crus- 
 tacea of North America, with remarks 
 on the order Phyllocarida. Pis. 1-38. 
 
 In Twelfth Rept. TJ. S. Geol. Survey Teiri- 
 tories (Hayden), Washington, 1883, pt. 1, p. 295. 
 
 Hymenocaris, Peltocaris, Oeratiocaris, Echi - 
 nocaris, Discinocaris, Spathiocaris, Lisgocaris , 
 Aptychopsis, Dictyocaris, Dithyrocaris, Ra- 
 chura, Argus, Estheria, Leaia. 
 
 Types of Carbouiferous X iphosura 
 
 new to North America. 
 
 In Am. Naturalist, vol. 19, 1885, p. 291.“ 
 
 Belinurus, Euproops, Oyclus, Dipeltis n. g. 
 
 The Syncarida, a group of Carbonif- 
 erous Crustacea. 
 
 In Am. Naturalist, vol. 19, 1885, p. 700. 
 
 Acanthotelson. 
 
VOGUES.] 
 
 LIST OF AUTHORS. 
 
 57 
 
 Packard, jr, (A. S.)— Continued. 
 
 On the Gampsonychidce , an unde- 
 scribed family of fossil Schizopod Crus- 
 tacea. 
 
 In Am. Naturalist, vol. 19, 1885, p. 790 ; Mem. 
 Nat. Acad. Sci., vol. 3, 1886, p. 129, pi. 3. 
 
 Palceocaris, Qampsonyx. 
 
 On the Anthracoridce, a family of 
 
 Carboniferous Alacrurous decapod Crus- j 
 tacea allied to the Eryovidw. 
 
 In Am. Naturalist, vol. 19, 1885, p. 880 ; Mem. 
 Nat. Acad. Sci , vol. 3, 1886, p. 135, pi. 4. 
 
 Anthrapalcemon. 
 
 Discovery of the thoracic feet in a 
 
 Carboniferous Phyllocaridan. 
 
 In Am. Philos. Soc., vol. 23, 1886, p. 380, plate. 
 
 Oryptozoe problematicus. 
 
 On the class Podostomata, a group 
 
 embracing the Merostomata and Trilo- 
 bites. 
 
 In Am. Naturalist, vol. 20, 1886, p. 1060. 
 
 Merostomata : Xiphosura, Synziphosura, Eu- 
 rypteridce. 
 
 On the Syncarida, a hitherto unde- 
 scribed synthetic group of extinct Ma- 
 lacostracous Crustacea. 
 
 In Mem. Nat. Acad. Sci., vol. 3, pt. 2, 1886, p. 
 123, pis. 1, 2. 
 
 Acanthotelson. 
 
 On the Carboniferous Xiphosurous 
 
 fauna of North America. 
 
 In Mem. Nat. Acad. Sci., vol. 3, pt.2, 1886, p. 
 143, 8 figs., 3 pis. 
 
 Cyclus, Dipeltis, Prestwichia, Belinurus, 
 Palceocaris, Anthrapalcemon, Protolimulus n. 
 g., Bunodes, Pseudoniscus, Exapinurus, Hemi- 
 aspis, Neolimulus. 
 
 Page (David). On the Pterygotus and 
 Pterygotus beds of Great Britain. 
 
 In Kept. 25th Meeting Brit. Assoc. Adv. Sci., 
 1855, Trans. Sec., p. 89. 
 
 The genus Stylonurus was proposed by Mr. 
 David Page in his paper read before the Asso- 
 ciation, and the name published in his “Ad- 
 vance text-book of geology,” 1856. 
 
 Further contributions to the palae- 
 ontology of the Tilestones or Silurio- 
 Devonian strata of Scotland. 
 
 In Kept. 28th Meeting Brit. Assoc. Adv. Sci., 
 Trans. Sec., p. 104. 
 
 Beyrichia, Oeratiocaris, Himantopterus, Sty- 
 lonurus tpinipes, S. clavipes, Kampecaris, Eu- 
 
 ryp torus. 
 
 Advance text-book of geology. Lon- 
 don, 1856. 
 
 Slimonia n. g., Stylonurus n. g., Kampecaris, 
 Himantopterus, Pterygotus, Parka. 
 
 Page (David) — Continued. 
 
 In the second edition, 1859, Mr. David Page 
 gives restorations of Pterygotus anglicus, Hi- 
 mantopterus acuminatus, Stylonurus powriei, 
 S. spinipes, Eurypterus clavipes, E. scouleri, and 
 Limulus rotundatus. 
 
 Note on the genus Stylonurus from 
 
 the Old Red Sandstone of Forfarshire. 
 
 In Proc. Royal Phys. Soc. Edinburgh, session 
 1864-’65, p. 230. 
 
 Pander (C. H.) Beitriige zur Geogno- 
 sie des russischen Reiches. St. Peters- 
 burgh, 1830 ; Leipzig, 1839, 31 pis. 
 
 Calymene, Asaphus, Illcenus, Nileus, Am- 
 phion n. g. , Zethus n. g. 
 
 Parkinson (James). Organic remains 
 of a former world, an examination of 
 the mineralized remains of the vege- 
 table and animal antediluvian world 
 generally termed extraneous fossils. 
 London, 1808, 3 vols. Crustacea, vol, 
 3, letter 16*, pi. 17. 
 
 Calymene, Ogygia, Encrinurus, Phacops, 
 Belinurus. 
 
 Payton. ( — ). Trilobites found in the 
 Transition limestone at Dudley, from 
 the collection of Mr. Payton, at Dudley. 
 London, 1827, 2 pp., 2 pis. 
 
 Calymene blumenbachii and Asaphus cau- 
 datus. 
 
 Peach (B. N.) On some new Crustaceans 
 from the Lower Carboniferous rocks of 
 Eskdale and Liddesdale. 
 
 In Trans. Royal Soc. Edinburgh, vol. 30, pt. 
 1, 1880, p. 73, 4 pis. 
 
 Oeratiocaris, Anthrapalcemon, Palceocran- 
 gon, Palceocaris, Uronetes. 
 
 Further researches among the Crus- 
 tacea and Arachnida of the Carbonif- 
 erous rocks of the Scottish border. 
 
 In Trans. Royal Soc. Edinburgh, vol. 30, pt. 
 2, 1880, p. 511, 2 pis. 
 
 Prestwichia, Cyclus, Eurypterus, Olyptoscor- 
 pius n. g., Acanthocaris n. g., Anthrapalcemon, 
 Palceocrangon, Palceocaris, Pseudo - Qalathea 
 n. g. 
 
 On the occurrence of Pterygotus and 
 
 a Limuloid in the Caithness Flagstones, 
 and on the nature and mode of forma- 
 tion of “Adam’s plate.” 
 
 In Proc. Royal Phys. Soc. Edinburgh, 1883, 
 p. 343, plate. 
 
 Pterygotus dicki. 
 
 Phillips (John). On the occurrence of 
 some minute fossil Crustaceans in Pa- 
 laeozoic rocks. 
 
 In Rept. 11th Meeting Brit. Assoc. Adv. Sci., 
 1841, Trans. Sec., p. 64. 
 
58 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 Phillips (John)— Continued. 
 
 Illustrations of the geology of York- 
 shire. Pt. 2. The mountain limestone 
 district. London, 1836, p. 239. 
 
 Asaphus ( Phillipsia ). 
 
 Figures and descriptions of the 
 
 Palaeozoic fossils of Cornwall, Devon, 
 and West Somerset, observed in the 
 course of the Ordnance Geological Sur- 
 vey of that district. London, 1841, 60 
 pis. Crustacea, p. 127. 
 
 Harpes, Calymene ( Ceraurus , Phacops), 
 Homalonotus, Asaphus, Bronteus. 
 
 The Malvern Hill compared with the 
 
 Palaeozoic district of Abberley, Wool- 
 hope, May Hill, Tortworth, and Usk. 
 
 In Mem. Geol. Survey Gt. Brit.,vol. 2, pt. 1, 
 London, 1848. Palaeontological appendix to 
 Prof. John Phillips’s memoir on the “ Malvern 
 Hills compared with the Palaeozoic district of 
 Abberley,” etc., by John Phillips and J. W. 
 Salter. Ibid., pp. 331-386, 30 pis. 
 
 For list of genera, see Salter (J. W.) and 
 Phillips ( J ohn). 
 
 Manual of geology. Pt. 2. Ed. by 
 
 Rob. Etheridge. 1885, pis. 1-12. 
 
 Paradoxides, Olenus , Asaphus, Ogygia, Caly- 
 mene, Trinucleus, Agnostus, Illsenus, Lichas, | 
 Beyrichia, Stygina, Phacops, Cybele , Cheirurus, 
 Bemopleur des, Harpes, Ampyx, Acidaspis, Cy- 
 phoniscus, JEglina, Sphcerexochus, Encrinurus, 
 Cyphaspis, Proetus, Pterygotus, Bronteus , 
 Homalonotus, Phillipsia. 
 
 Pictet (F.-J.) TraitA de pal^ontologie, 
 ou histoire naturelle des animaux fos- 
 siles consider As dans leurs rapports 
 zoologique et g^ologique. 4 vols and 
 atlas. Paris, 1853-’57. Crustacea, vol. 
 2, 1854, p. 413. 
 
 The author arranges the families and genera 
 as follows: Harpidae: Harpes. Paradoxidae: 
 Bemopleurides, Paradoxides, Hydrocephalus, 
 Sao, Arionellus, Ellipsocephalus, Olenus, Pel- 
 tura, Triarthrus, Conocephalites. Caiymeuidae, 
 1st section, Proetidae : Proetus, Phillipsia, Cy- 
 phaspis, Arethusina, Harpes ; 2.1 section, Pha- 
 copidaB : Phacops, Dalmania ; 3d section, Caly- 
 menid&e: Calymene, Homalonotus. Lichasidae. 
 Lichas. Trinucleidae: Trinucleus, Ampyx, Dio- 
 nide. Asaphidae : Asaphus, Symphysurus, 
 Ogygia. iEglinidae: JEglina. Illaenidae: lllce- 
 nus, Nileus. Odontopleuridae : Acidaspis, Chei- 
 rurus, Placoparia, Sphcerexochus, Staurocepha- 
 lus, Deiphon, Zethus, Dindymene. Amphioni- 
 dae : Amphion, Cromus, Encrinurus. Bronti- 
 dae : Bronteus. Agnostidae : Agnostus. Phyllo- 
 podae : Apusiens, Dithyrocaris, Apus, Estheria, 
 Copepodae : Eurypterus. Cypi’oidaB : Cythere, 
 Bairdia, Beyrichia, Leperditia, Cypris. Cypri- 
 dinae : Cyprella, Oypridella. Xiphosurae : Li- 
 mulus, Belinurus, Pterygotus. Amphipodae : 
 Qampsonyx. 
 
 Pitt. See Grote and Pitt. 
 
 Plant (John). On the discovery of Para- 
 doxides davidis at Tyddyngwladis, near 
 Dolgelly, North Wales. 
 
 In Trans. Manchester Geol. Soc., vol. 5, 1886, 
 p. 76. 
 
 Pohlman (Julius). On certain fossils of 
 the Waterlime group near Buffalo. 
 
 In Bull. Buffalo Soc. Nat. Sei., vol. 4, 1881, p. 
 17, 7 figs. 
 
 Pterygotus buffaloensis, Ceratiocaris grandis. 
 
 Additional notes on the fauna of the 
 
 Waterlime group. 
 
 In Bull. Buffalo Soc. Nat. Sci., vol. 4, 1882, p. 
 41, 2 pis. 
 
 Eurypterus giganteus, Pterygotus globicauda- 
 tus, P. acuticaudatus, P. quadraticaudatus, P. 
 macrophthalmus?, P. buffaloensis. 
 
 Fossils from the Waterlime gtoup 
 
 near Buffalo, N. Y. 
 
 In Bull. Buffalo Soc. Nat. Sci., vol. 5, 1886, p. 
 17, pi. 3. 
 
 Pterygotus buffaloensis, P. bilobus, Ceratioca- 
 ris acuminatus, Eusarcus, E. grandis, Eurypte- 
 rus scorpionis (the term Eurypterus scorpioe- 
 des was used by Henry Woodward for a species 
 of this genus in 1868. See Eurypterus pohl- 
 mani). 
 
 Portlock (J. E.) Report on the geology 
 of the county of Londonderry, and of 
 parts of Tyrone and Fermanagh. Dub- 
 lin, 1843, 28 pis., also maps and sections. 
 
 Harpes, Bemopleurides n. g., Proetus, Phillip- 
 sia n. g., Griffithides n. g., Phacops, Calymene, 
 ges, Trinucleus, Ampyx, Nuttainia, Asaphus, 
 Isotelus, Ogygia, Ceraurus, Amphion, Zethus, 
 Brontes, lllcenus, Dithyocaris (Seoul er) Port- 
 lock, Limulus. 
 
 Postlethwaite (J.) and Goodchild (J. 
 G.) On some Trilobites from the Skid- 
 daw slates. 
 
 In Proc. Geologist Assoc., vol. 9, No. 7, 1886, 
 p. 455, pis. 6-9. 
 
 In this contribution the initials of each au- 
 thor designate the paragraphs written by him. 
 
 The following list is given of the Trilobite 
 fauna of the Skiddaw slates : 
 
 Phacops nicholsoni Salter, Cybele ovata Ether- 
 idge, Calymene brevicapitata ? , Bemopleurides 
 sp. ? , Olenus sp. ? , Trinucleus gibbsii ?, Ogygia 
 selwyni, Ogygia sp. ?, Barrandia falcata P. & 
 G., Niobe doveri Eth., Eurymetopus cambrianus 
 n. g. and n. sp. P. & G., E.harrisonii P. A G., 
 JEglina? rediviva Barr., A. binodosa, A. obtu- 
 sicauda Hicks, A.? caliginosa, Agnostus .morei 
 Salter. 
 
 Prestwich (S.) On the geology of Coal- 
 brook Dale. 
 
 In Trans. Geol. Soc. London, vol. 5, 1840, p. 
 413, map, 2 sections, 4 pis. 
 
 Belinurus. 
 
V0GDES.1 
 
 LIST OF AUTHORS. 
 
 59 
 
 Quenstedt (F. A.) Beitrage zur Kennt- 
 niss der Trilobiten. Riicksicht auf ihre 
 bestimmte Gliederzahl. 
 
 In Arcliiv fiir Naturgesch. (Wiegmann), 
 vol. 1, Berlin, 1837, p. 337. 
 
 In this work Prof. F. A. Quenstedt divides 
 the Trilobites into two groups: 1. Trilobites 
 with faceted eyes; 2. Trilobites with non- 
 faceted eyes. The genera are classified accord- 
 ing to the number of segments in the thorax. 
 
 Rafinesque (C. S.) On the genera of fos- 
 sil Trilobites or Glomerites of North 
 America. 
 
 In Atlantic Jour, and Friend to Knowledge, 
 vol. 1, 1832, p. 71. 
 
 Ramsay (A. C.) The geology of North 
 Wales, with an appendix on the fossils; 
 with plates by J. W. Salter. 
 
 In Mem. Geol. Survey Gt. Brit., vol. 3, 1866. 
 
 Di/celocephalus, Olenus, Parabolina, Cono- 
 coryphe, Angelina , Homalonotus, Lichas, Trinu- 
 cleus, Dionide, Ampyx, Asaphus, Kiobe, JEglina, 
 Cheirurus , Encrinurus , lllcenus, Agnostus, Psi- 
 locephalus, Beyrichia, Hymenocaris. 
 
 Rathbun (Richard). See Hartt (C. F.) 
 and Rathbun (Richard). 
 
 Ratte (F.) Note on some Trilobites new 
 to Australia. 
 
 In Proc. Linn. Soc. New South Wales, 2d 
 series, vol. 1, 1886, p. 1067, 3 pis. 
 
 Lichas, Proetus, Acidaspis. 
 
 Note on some Trilobites new to Aus- 
 tralia. 
 
 In Proc. Linn. Soc. New South Wales, 2d 
 series, vol. 2, 1887, p. 95, 2 pis. 
 
 Lichas, Acidaspis, Staurocephalus. 
 
 Razoumowsky ( Comte de ). Quelques 
 observations sur les Trilobites et leurs 
 gisements. 
 
 In Annales Sci. Nat. Paris, vol. 8, 1826, p. 186. 
 
 Trilobites de Zarsko silo. 
 
 Remete (A.) Kataloge der Geschiebe- 
 sammlung. Berlin, 1885. (*) 
 
 Reuss (A. E.) Entomostraca and Fora- 
 minifera of the Zechstein of the Wet- 
 terau. Plate. 
 
 In Jahresbericht der wetterauischen Gesell. 
 fiir die gesammte Naturk., 1854, p. 59 (Hanau). 
 
 Palteontologische Miscellen. 
 
 In Denkschriften k. Akad. Wiss. Wien, vol. 
 10, 1856, 7 pis. 
 
 Lepidoderma n. g., Lepidodenna imhoffi. 
 
 This genus is referred by H. Woodward to 
 the genus Eurypterus. 
 
 Reuss (F.) Geognostische Bemerkungen 
 auf einer Reise durch einen Ti.eil des 
 Pilsner Kreises. 
 
 In Sammlnng naturhist. Aufsatze, vol. 4, 
 
 1794, p. 47. 
 
 | Reuter (G.) Die Beyrichien der obersilu- 
 rischen DiluvialgeschiebeOstpreussens. 
 
 In Zeitschr. Deutsch geol. Gesell., Berlin, 
 vol. 37, 1885, p. 621, pis. 25, 26. 
 
 Richter (R.) Beitrage zur Palaeoutolo- 
 gie Thiiringens. Leipzig, 1848, 6 pis. 
 
 Aus dern thiiringischen Zechstein. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 7, 1855, p. 526. 
 
 Gythere, Cytherella, Cythereis, Bairdia. 
 
 Aus dem thiiringischen Schiefe-ge- 
 
 birge. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 15, 1863, p. 659, 2 pis. 
 
 Harpes, Proetus , Arethusina, Phyllaspis n. 
 g. , Phacops, Acidaspis, Beyrichia. 
 
 Aus dem thiiringischen Schieferge- 
 
 birge. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 17, 1865, p. 361, 2 pis. 
 
 Proetus expansus, P. plagiophthalmus, Chei- 
 rurus, Beyrichia klodeni, B. subcylindria. 
 
 Das thiiringische Schiefergebirge. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 21,-1869, p. 341. 
 
 Proetus, Phacops, Dalmanites. 
 
 Devonische Entomostraceen in Thii- 
 
 ringen. 
 
 In Zeitschr. Deutsch. geol. Ges.ell., Berlin, 
 vol. 21, 1869, p. 757, pis. 20, 21. 
 
 Beyrichia, Cypridina, Cytherina. 
 
 Roberg (L.) Dissertatio academica de 
 fluviatile Astaco, etc. Upsalise, 1715. 
 
 This work contains a plate with the figure of 
 the pygidia of Trilobites and a fossil Crusta- 
 cean. Fig. H is of a large pygidiuru of some 
 species of Asaphus. Fig. J is a cast in stone 
 of a smaller species of the same genus. The 
 author remarks “that he found the specimens 
 during an excursion along the shores of the 
 Baltic Sea, in a red limestone.” He has the 
 merit of referring these fossils to the class 
 Crustacea. 
 
 Roemer (F. A. ) Versteinerungen der 
 Hartzgebirge. Hannover, 1843, 12 pis. 
 Crustacea, p. 37. 
 
 Brontes flabellifcr, B. signatus, B. ? glabra- 
 tus, Calymene? jo rdoni, C. schusteri, C sub- 
 ornatus , C. hydrocephala, Asaphus zinckeni, 
 Paradoxides grotei, Homalonotus ahrendi, H. 
 punctatus, H. gigas. 
 
 Roemer (Ferdinand). Beitrage zur ge- 
 ologischen Kenntniss des nordwest- 
 liclien Harzgebirges. 
 
 In Palajontographica, vols. 3, 5, and 13, 5 pts., 
 Cassel, 1854-’66, 38 pis. 
 
 Conoccphalus , Proetus, Cyphaspis, Phacops, 
 Trimerocephalus, Homalonotus. Lichas, Bron- 
 teus, Acidaspis, Trochus, Cheirurus , Dithyro- 
 caris, Cypridina, Harpes, Phillipsia. 
 
60 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63. 
 
 Roemer (Ferdinand)— Continued. 
 
 Das rheinische Uebergangsgebirge, 
 
 eine palseontologisch - geognostische 
 Darstellung. Hannover, 1844, pi. 2. 
 
 Phacops latifrons, Pleuracanthus acimatus, 
 P. punctatus, Gerastos Icevigatus. 
 
 Texas, mit besonderer Riicksicht 
 
 anf deutscbe Auswanderung und die 
 pbysischen Verhiiltnisse des Landes, 
 nach eigener Beobachtung gescbildert. 
 Mit einem naturwissenschaftlichen 
 Anbange und einer topographisch- 
 geognostischen Karte von Texas. 
 Bonn, 1849. 
 
 In the list of fossils on p. 421 Pterocephalia 
 sancti sabce Roemer is mentioned. 
 
 Ueber ein bisher nicbt bescbriebenes 
 
 Exemplar von Eurypterus aus devoni- 
 scben Schichten des New York. 
 
 In Palaeontographica, vol. 1, 1851, p. 190. 
 
 Die Kreidebildung von Texas. 
 
 Bonn, 1852, 11 pis. 
 
 Pterocephalia sancti sabce n. g. and sp. 
 
 Notiz tiber eine riesenhafte neue Art 
 
 der Gattnng Leperditia in silurischen 
 Diluvial-Geschieben Ost-Preussen’s. 
 
 In Zeitschr. Deutsch. geol. Gesell , Borlin, 
 vol. 10, 1858, p. 356, 2 figs. 
 
 Leperditia baltica, L. gigantea. 
 
 Die Yersteinerungen der silurischen 
 
 Diluvial-Geschiebe von Groningen in 
 Holland. 
 
 In Neues Jahrbuch fiir Mineral., 1858, p. 257. 
 
 Proetus , Encrinurus, Beyrichia, Cytherina. 
 
 Die Silurische Fauna des westlichen 
 
 Tennessee. Breslau, 1860, 5 pis. 
 
 Dalmania , Calymene, Ceraurus, Sphcerexo- 
 chus, Bumastus. 
 
 Palseo - lethsea. II. Theil: Kohlen- 
 
 Periode (Silur-, Devon-, Kohlen- und 
 Zechstein-Formation). 
 
 In Bronn’s Lethsea geognostica, etc., Stutt- 
 gart, 1851-’56. 
 
 For list of genera, see Broun (H. G.) and 
 Roemer (F.) Lethsea geogn. 
 
 Bericht Uber eine geologische Reise 
 
 nach Norwegen im Sommer 1859. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 11, 1860. 
 
 Dalmania, Cryphceus, Asaphus, Illcenus, 
 Phacops. 
 
 Die fossile Fauna der silurischen 
 
 Diluvial-Geschiebe von Sadewitz bei 
 Oels in Niederschlesien. Breslau, 1861, 
 8 pis. 
 
 Ceraurus, Remopleurides, Isotelus , Asaphus, 
 Illcenus, Chasmops, Proetus , Calymene, Encri- 
 nurus, Lichas. 
 
 Roemer (Ferdinand) — Continued. 
 
 Ueber die Diluvial-Geschiebe von 
 
 nordischen Sedimentar - Gesteinen in 
 den norddeutschen Ebene etc. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 14, 1862, p. 575. 
 
 Beyrichia. 
 
 Ueber eine marine Conchylien-Fauna 
 
 im productiven Steinkohlengebirge 
 Oberschlesiens. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 15, 1863, p. 567, pis. 14-16. 
 
 Griffithides mesotuberculata McCoy, Phillip- 
 sia. 
 
 Notiz uber das Yorkommen von 
 
 Eurypterus scouleri im niederschlesi- 
 schen Steinkohlengebirge. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 25, 1873, p. 562, 1 fig. 
 
 Lethsea palaeozoica. Stuttgart, 1880. 
 
 Text and atlas. 
 
 Ueber die Gattung Arthropleura aus 
 
 dem schlesischen Steinkohlengebirge. 
 
 In Sitzungsber. schles. Gesell. fiir vaterland. 
 Cultur, Breslau, Jahrg. 1880, p. 128. 
 
 Ueber eine Kohlenkalk-Fauna der 
 
 Westkiiste von Sumatra. Cassel, 1880, 
 3 pis. 
 
 Phillipsia sumatrensis Roemer. 
 
 Ueber eine Art der Limuliden-Gat- 
 
 tung Belinurus aus dem Steinkohlenge- 
 birge Oberschlesien’s. 
 
 In Zeitschr. Deutsch. geol. Gesell., Berlin, 
 vol. 35, 1883, p 429, 2 figs. 
 
 Lethsea erratica, oder Aufzahlung 
 
 und Beschreibung der in den nord- 
 deutschen Ebene vorkommenden Di- 
 luvial Geschiebe nordischen Sedimen- 
 tar-Gesteine. Berlin, 1885, 11 pis. 
 
 In this work many Trilobites and other 
 Crustacea are mentioned, but only a few new 
 species are figured. 
 
 Rogers (\Y. B.) Discovery of Paradoxi- 
 des in the altered rocks of Massachu- 
 setts. 
 
 In Edinb. New Philos. Jour., vol. 4, 1856. 
 
 On the discovery of Cambrian fossils 
 
 at Braintree, Mass. 
 
 In Proc. Boston Soc. Nat. Hist., vol. 5, 1854, 
 p. 27 (continued on p. 40). 
 
 Paradoxides harlani Green. 
 
 Paradoxides near Boston. 
 
 In Edinb. New Philos. Jour., vol. 6, 1857, p. 
 314. 
 
 Rogers ( Henry D. ) The geology of 
 Pennsylvania. A Government survey 
 with a general view of the geology 
 
V0GDE8-] 
 
 LIST OF AUTHORS. 61 
 
 Rogers (Henry D.) — Continued, 
 of the United States, essays on the coal 
 formation and its fossils, and a descrip- 
 tion of the coal fields of North America 
 and Great Britain. 2 vols. Edin- 
 burgh, London, and Philadelphia, 1858. 
 Atlas of plates and maps. 
 
 Organic remains of the Palaeozoic strata of 
 Pennsylvania, vol. 2, pp. 815-834. 
 
 Paradoxides, Asaphus, Calymene. 
 
 Notes on the Beyrichia and Leperditia, by T. 
 Rupert Jones, vol. 2, p. 834, figs. 595-699. 
 
 Rominger (C.) Description of Primor- 
 dial fossils from Mount Stephens, N. W. 
 Territory of Canada. 
 
 In Proc. Acad. Nat. Sci. Phila., 1887, p. 12, 
 
 lpl. 
 
 Ogygia, Embolimus n. g , Menocephalus, 
 Conocephalites, Bathyurus ?, Agnostus. 
 
 Dr. C. RomingeFs rejoinder to Mr. 
 
 C. D. Walcott. 
 
 In Am. Geologist, vol. 2, 1888, p. 356. 
 
 Rouault (Marie). Mdmoire sur les Trilo- 
 bites du d^partement d’llle et-Vilaine. 
 
 In Bull. Soc. G6ol. Prance, 2d series, vol. 4, 
 1846, p. 309. 
 
 Trinucleu8, Nileus, Prionocheilus n. g., Caly- 
 mene, Phacops, Polyeres, Cheirurus, Trinucleus. 
 
 M6moire. 1. Sur la composition du 
 
 test des Trilobites. 2. Sur les change- 
 ments de formes dus k des causes acci- 
 dentelles, ce qui a pu permettre de con- 
 fondre des esp&ces diffdrentes. 
 
 In Bull. Soc. G6ol. France, vol. 6, 1848, p. 67, 
 pis. 1-2. 
 
 Ogygia brongniarti, O. edwardsi, Illcenus des- 
 maresti, Calymene arago, Trinucleus. 
 
 Fossiles du terrain silurien, dtage 
 
 du schiste, ardoisier fosillif&re, Crus- 
 tac6s, famille des Trilobites. 
 
 In Bull. Soc. G6ol. Prance, vol. 8, 1851, p. 358. 
 
 Calymene salteri, O. verneuili, Dalmannia 
 vetillarti, D. incerta, Placoparia tournemini , 
 Ogygia desmaresti, Homalonotus brongniarti , 
 H. barrandei, H. hausmanni , IT. legraverendi, 
 Plcesiacomia kieneria, Proetus huhayi, P. mi- 
 chelini, Cyphaspis , Beyrichia, Leperditia n. g., 
 L. britannica, Phacops. 
 
 Safford (J. M.) Geology of Tennessee. 
 Nashville, 1869, 7 pis. and map. 
 
 The author, in his catalogue of Trenton 
 and Nashville fossils occurring in the Central I 
 Basin, p. 285, gives the names of Dalmanites j 
 troosti n. s. and Encrinurus excedrinua n. s., but 
 without specific descriptions. 
 
 Sandberger (G.) and Sandberger (F.) J 
 Die Versteiueruugen des rheinischen i 
 Schichten -System in Nassau. Wiesba- I 
 den, 1850- 56, atlas in folio, 39 pis. 
 
 Sandberger (G ) and Sandberger (F.)— 
 Continued. 
 
 Harpes, Cyphaspis, Trigonaspis n. g., Cylin- 
 draspis n. g., Phacops, Dalmanites, Homalono- 
 tus, Odontopleura, Cheirurus, Bronteus, Cyprin- 
 dia. 
 
 Salter (J. W.) On the structure of Tri- 
 nucleus , with remarks on other species. 
 
 In Quart. Jour. Geol. Soc. London, vol. 3, 
 1847, p. 251, 4 figs. 
 
 Crustacea. 
 
 In Mem. Geol. Survey Gt. Britain, vol. 2, pt. 
 1, 1848, pp. 333-352, figure, pis. 5-8. 
 
 Olenus , Proetus, Phacops, Dalmannia, Caly- 
 mene, Lichas, Trinucleus, Ampyx, Ogygia, Illce- 
 nus, Acidaspis, Cheirurus, Sphcerexochus, Gy- 
 bele, Agnostus, Beyrichia. 
 
 and Forbes (Edward). Figures and 
 
 descriptions illustrative of British or- 
 ganic remains. Decade 2. 
 
 In Mem. Geol. Survey United Kingdom Lon- 
 don, 1849, 10 pis. 
 
 Paradoxides, Olenus, Parabolina n. g., Pha- 
 cops, Dalmannia, Portlockia, Cryphceus, Caly- 
 mene, Ampyx, Brachampyx n. g., Asaphus, 
 Ogygia, Illcenus, Bumastus. 
 
 The description of all the species, with the 
 exception of Ampyx nudus, was made by J. W. 
 Salter. 
 
 Description of Pterygotus problemati- 
 
 cus Agass. 
 
 In Quart. Jour. Geol. Soc. London, vol. 8, 
 1852, p. 386, pi. 21. ’ 
 
 Pterygotus, Bellinurus. 
 
 Appendix A to British Palaeozoic 
 
 fossils in the Geological Museum, Uni- 
 versity of Cambridge. London, 1852 
 (Sedgwick and McCoy). 
 
 Description of a few species from Wales and 
 Westmoreland, referred to in the foregoing 
 work by John William Salter, p. 645. 
 
 Phacops, Calymene, Homalonotus, Lichas, 
 Illcenus, Cheirurus, Encrinurus, Cybele, Bey- 
 richia, Cythere, Eurypterus. 
 
 On the lowest fossiliferous beds of 
 
 North Wales. 
 
 In Rept. 22d Meeting Brit. Assoc. Adv. Sci., 
 1852, Trans, of Sec., p. 56. 
 
 Hymenocaris n. g. 
 
 On a few genera of Irish Silurian 
 
 fossils. 
 
 In Rept. 22d Meeting Brit. Assoc. Adv. Sci., 
 1852, Trans, of Sec., p. 59. 
 
 Stygina n. g., Cyphoniscus n. g., Remopleuri- 
 des, Cyphaspis, JEglina, Acidaspis. 
 
 Notes on the Trilobites. 
 
 Appendix C to an article by Senhor Carlos 
 Ribeiro on the Carboniferous and Silurian for- 
 mations of the neighborhood of Bussaco, in 
 Portugal. 
 
62 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 63. 
 
 Salter (J. W.) — Continued. 
 
 In Quart. Jour. Geol. Soc. London, vol. 9. 
 1853, p. 158, pi. 7. 
 
 Phacops, Calymene, Trinucleus, Ogygia, Illce- 
 nus, Placoparia. 
 
 On Arctic Silurian fossils. 
 
 In Quart. Jour. Geol. Soc. London, vol. 9, 
 853, p. 312. 
 
 Proetus, Encrinurus, Leperditia. 
 
 Figures and descriptions illustrative 
 
 of British organic remains. Decade 7. 
 
 In Mem. Geol. Survey United Kingdom, Lon- 
 don, 1853, 10 pis. 
 
 The genera are arranged in this work in the 
 following order: 1. Phacops downingice, section 
 Acaste, P. apiculatus, P. brongniarti, P. dal- 
 manni , P. jamesii, P. alifrons, P. jukesii, P. 
 conophthalmus section Oilontochile ( Dalman - 
 nia), P. mucronatus, P. amphora. 2. Cheirurus 
 bimucronatus, section Crotalocephalus, C. arti- 
 culatus?; section Cheirurus, O.speciosus, C.ge- 
 lasinosus, C. cancrurus, C. octolobatus ; section 
 Actinopeltis, (7. clavifrons. 3. Sphcerexochus 
 mirus. 4. Encrinurus sexcostatus, E. puncta- 
 tus , E. variolaris, E. multisegmentatus. 5. 
 Cyphaspis megalops, C. pygmceus 6. Acidaspis 
 jamesii, A. bispinosus, A. caractaci. 7. Trinu- 
 cleuslloydii, section 1, Trinucleus proper, T. con- 
 centricus, with four varieties, T. thersites ; sec- 
 tion 2, Tretaspis, T. seticornis , T. fimbriatus, T. 
 radiatus. 8. R emopleurides colbii, R. laterispi- 
 nifer , R. dorsopinifer section Remopleurides, 
 R.platyceps , R. longico status, R. obtusus ; sec- 
 tion 2, Caphyra , R. (Caph.) radians. 9. Cypho- 
 niscus socialis. 10. JEglina mirabilis, JEglina 
 major. 
 
 
 On some new Crustacea from the 
 
 uppermost Silurian rocks, by J. W. 
 Salter. With a note on the structure 
 and affinities of Himantopterus, by T. 
 H. Huxley. 
 
 In Quart. Jour. Geol. Soc. London, vol. 12, 
 1856, pi. 26, figs. 1-7. 
 
 Himantopterus n. g. 
 
 Description of the Crustaceans from 
 
 the uppermost Silurian rocks near Les- 
 inahago. 
 
 In London, Edinb., Dublin Philos Mag., vol. 
 11, 1856, p. 83. 
 
 Himantopterus. 
 
 On the great Pterygotus (Seraphim) 
 
 of Scotland and other species. 
 
 In Rept. 26th Meeting Brit. Assoc. Adv. Sci., 
 1856, Trans, of Sec., p. 75. 
 
 On fossil remains in the Cambrian 
 
 rocks of the Longmynd and North 
 Wales. 
 
 In Quart. Jour. Geol. Soc. London, vol. 12, 
 1856, p. 246. 
 
 Palceopyge ramsayi, pi. 4, fig.. 3, new species 
 and genus. 
 
 Salter (J. W.) — Continued. 
 
 On two Silurian species of Acidaspis 
 
 from Shropshire. 
 
 In Quart. Jour. Geol. Soc. London, vol. 13, 
 1857, p. 210, pi. 6. 
 
 On some new species of Eurypterus. 
 
 With note on the distribution of the 
 species. 
 
 In Quart. Jour. Geol. Soc. London, vol. 15, 
 1859, p. 229, pi. 10. 
 
 On the fossils of the Lingula flags 
 
 or zone Primordiale Paradoxides and 
 Conocephalus from North America. 
 
 In Quart. Jour. Geol. Soc. Loudon, vol. 15, 
 1859, p. 551, 4 figs. 
 
 Paradoxides bennetti, Conocephalus antiqua- 
 tus, Asaphus or Olenus sp. ? 
 
 New Silurian Crustacea. 
 
 In Annals Mag. Nat. Hist., 3d series, Lon- 
 don, vol. 5, 1860, p, 153, figures. 
 
 Geratiocaris , Dictyocaris n. g., Physocaris 
 n. g. 
 
 On the fossils from the High Andes, 
 
 collected by David Forbes. 
 
 In Quart. Jour. Geol. Soc. London, vol. 17, 
 1861, p. 62, pis. 4, 5. 
 
 Proetus ( Cryphceus ) pentlandi , Homalonotus 
 linares, H. sp. ? , Beyrichia forbesii, Phacops lati- 
 frons Bronn. 
 
 On some of the higher Crustacea 
 
 from the British Coal Measures. 
 
 In Quart. Jour. Geol. Soc. London, vol. 17, 
 1861, p. 528, figs. 1-8. 
 
 Anthrapalaemon n. g., Palceocrangon n. g. 
 
 Name changed to that of Crangopsis. See 
 same journal, vol. 19, p. 80. 
 
 Crustacea in the Coal Measures. 
 
 In London, Edinb., Dublin Philos. Mag., vol. 
 22, 1861, p. 325. 
 
 Anthrapalcemon. 
 
 This is merely a notice of the article referred 
 to in the Quart. Jour. Geol. Soc., vol. 17, 1861, p. 
 528. 
 
 Description of Uronectes (Gamponyx) 
 
 socialis in the Rev. T. Brown’s paper, 
 “Mountain limestone and Lower Car- 
 boniferous rocks of the Fifeshire 
 coast.” (*) 
 
 In Trans. Royal Soc. Edinb., vol. 22, pt. 2, 
 1861, p. 394. 
 
 A monograph of British Trilobites. 
 
 In Palaeont. Soc. London, vol. 16, 1862, pp. 
 1-83, pis. 1-6, pt. 1. 
 
 Phacops, subgenera Trimerocephalus McCoy , 
 Phacops Emm. , Acaste Gold., Ohasmops McCoy, 
 Odontochile Corda, Cryphceus Green. 
 
 Cheirurus, subgenera Crotalocephalus Sal- 
 ter, Oheirurus Beyrich, Eccoptochile Corda, 
 Actinopeltis Corda, Sphcerexochus Beyrich, 
 
 Amphion Pander. 
 
V0GDE8.] 
 
 LIST OF AUTHORS, 
 
 63 
 
 Salter (J. W.)— < Continued. 
 
 On some fossil Crustacea from tlie 
 
 Coal Measures and Devonian rocks of 
 New Brunswick, Nova Scotia, and Cape 
 Breton. 
 
 In London, Edinb., Dublin Philos. Mag., 4th 
 series, vol. 24, 1862, p. 166. 
 
 A monograph of British Trilobites. 
 
 Pt. 2. Pp. 81-128, pis. 7-19. 
 
 In Palaeont. Soc. London, vol. 17, 1863. 
 
 Calymene, Momalonotus, subgenera Bron- 
 gniartia Salter (not Brongniartia Eaton), Tri- 
 merus Green, Dipleura Green, Koenigia Salter, 
 Burmeisteria Salter; Ogygia, Staurocephalus, 
 Deiphon, Amphion. 
 
 On some fossil Crustacea from the 
 
 Coal Measures and Devonian rocks of 
 British North America. 
 
 In Quart. Jour. Geol. Soc. London, vol. 19, 
 1863, p. 75, figs. 1-12. 
 
 Amphipeltis n. g., Diplostylus n. g., Eurypte- 
 rus, Palceocrangon. 
 
 The author herein changes the name Palceo- 
 crangon Salter to that of Crangopsis. 
 
 On some species of Eurypterus and 
 
 allied forms. 
 
 In Quart. Jour. Geol. Soc. London, vol. 19, 
 1863, p. 81, 8 wood-cuts. 
 
 Eurypterus scouleri, E. (Arthropleura?) 
 mammatus, E. ? (Arthropleura) ferox. 
 
 On Peltocaris, a new genus of Silu- 
 rian Crustacea. 
 
 In Quart. Jour. Geol. Soc. London, vol. 19, 
 1863, p. 87. 
 
 Peltocaris n. g., Hymenocaris, Geratiocaris, 
 Dictyocaris, Dithyrocaris, Arges, Apus, Nebalia, 
 Estheria, Leperditia, Beyrichia. 
 
 On some tracks of Lower Silurian 
 
 Crustacea. 
 
 In Quart. Jour. Geol. Soc. London, vol. 19, 
 1863, p. 92, figures. 
 
 Note on the Skiddaw slate fossils. 
 
 In Quart. Jour. Geol. Soc. London, vol. 19, 
 1863, p. 135, figures. 
 
 Caryocaris n. g. 
 
 On the discovery of Paradoxides in 
 
 Britain. 
 
 In Quart. Jour. Geol. Soc. London, vol. 19, 
 1863, p. 274. 
 
 Paradoxides davidis. 
 
 On a new Crustacean from Glasgow 
 
 Coal Field. 
 
 In Quart. Jour. Geol. Soc. London, vol. 19, 
 1863, p. 519, figs. 1, 2. 
 
 Palceocarabus russellianus. 
 
 A monograph of British Trilobites. 
 
 Pt. 3. Pp. 129-179, pis. 15-25. 
 
 In Palmont. Soc. London, vol. 18, for 1864 
 (London, 1866). 
 
 Salter (J. W.) — Continued. 
 
 Ogygia , subgenera Barrandia, and Homalop- 
 teon ; Niobe , Asaphus, subgenera Ptychopyge, 
 Basilicus, Mcgalaspis, Isotelus, Cryptonymus, 
 Symphysurus, Brachyaspis, and Nileus ; Sty- 
 gina, Psilocephalus n. g. 
 
 Figures and descriptions illustrative 
 
 of British orgauic remains. Decade XI. 
 Trilobites (chiefly Silurian). 
 
 In Mem. Geol. Survey United Kingdom, Lon- 
 don, 1864, 10 pis. 
 
 Paradoxides , Angelina , Olenus, O. ( Lepto - 
 plastus), O. ( Peltura ), O. ( Splicer ophthalmus), 
 O. ( Parabolina ), Conocoryphe, Phacops (Tri- 
 merocephalus), Salteria n. g., Stygina, Asaphus, 
 JEglina, Staurocephalus , Agnostus, A. ( Condy - 
 lopyge), A. (Trinodus), A. (Phalacroma). 
 
 The article on Salteria primceva n. g. et sp., 
 pi. 6, was edited by P. Wj ville Thomson. 
 
 On some fossils from the Lingula 
 
 flags of Wales. 
 
 In Quart. Jour. Geol. Soc. London., vol. 20, 
 1864, p. 233, pi. 13. 
 
 Paradoxides, Anopolenus n. g., Conocoryphe, 
 Holocephalina n. g., Microdiscus, Agnostus, 
 Leperditia . 
 
 Note on the fossils from the Budleigh 
 
 Sandstone Pebble bed. 
 
 In Quart. Jour. Geol. Soc. London, vol. 20, 
 1864, p. 286, pi. 15. 
 
 Phacops incertus, Calymene tristani, Soma- 
 lonotus brongniarti, Myocaris n. g. 
 
 For detailed description of Myocaris, see 
 Geol. Mag., vol. 1, London, 1864, p. 11, fig. 4. 
 
 On the new genus Anopolenus. 
 
 In Geol. Mag., vol. 1, London, 1864, p. 6. 
 
 Anopolenus n. g., Myocaris. 
 
 Catalogue of the Museum of Practi- 
 cal Geology of London. London, 1865. 
 
 and Woodward (Henry). Chart 
 
 of fossil Crustacea, accompanied by a 
 descriptive catalogue of all the genera 
 and species figured. London, 1865, 
 pis. 3 and 4. 
 
 Permian : Prosopiniscus, Dcdmanites ? ka- 
 bliktce, Estheria, Kirkbya, Bairdia, Cythcrideis, 
 Cythere, Limulus. 
 
 Coal : Palceocarabus, Pygocephalus, TJronectus 
 (Gampsonyx), Diplostylus, Phillipsia, Estheria, 
 Beyrichia, Kirkbya, Leperditia, Oandona, Leaia, 
 Arthropleura, Eurypterus, Limulus ? (Bclinu- 
 rus). 
 
 Mountain Limestone: Palceocrangon , Brachy- 
 metopus, Grijffithides, Phillipsia, Dithyrocaris, 
 Cyclus, Estheria, Cythere, Gypridina, Cyprella, 
 Cypridella, Entomoconchus, Beyrichia, Bairdia, 
 Leperditia, Eurypterus, Limulus 1 trilobitoides. 
 
 Devonian : Amphipeltis, Gilocrangon, Campe- 
 caris, Proetus, Encrinurus, Bronteus, Phacops, 
 Oyphaspis, Arges, Typhomiscus, Uomalonotus, 
 JIarpes, Cypridina, Esther ia, Leperditia, Ento - 
 
64 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [uull. 63. 
 
 Salter (J. W.)— Continued. 
 
 mis, Gypridina, Beyrichia, Bostrichopus , Eu- 
 rypterus, Pterygotus. 
 
 Upper Silurian: Bronteus, lllcenus, Cyphas- 
 pis, Proetus, Aulacopleura, Phacops, Encri- 
 nurus, Acidaspis, Cheirurus, Homalonotus, Dei- 
 phon, Calymene, Harpes, Dictyocaris, Beyrichia , 
 Ceratiocaris, Leperditia, Stylonurus, Pterygotus, 
 Hemiaspis, Slimonia, Bunodes. 
 
 Lower Silurian: Asaphus, Stygina, Nileus , 
 lllcenus, AEglina, Ogygia, Agnostus, Niobe, Pha- 
 cops, Trinucleus, Ampyx, Sphcerexochus , Dio- 
 nide, Eccoptochile, Placoparia, Lichas, Oybele , 
 Acidaspis, Calymene, Staurocephalus, Jtemo- 
 pleurides, Gyphoniscus, Atops, Triarthrus, Gory 
 nexochus, Centropleura, Monocephalus, Pelto- 
 caris, Beyrichia, Cytheropsis, Protichnites. 
 
 Cambrian : Agnostus, Sao, Anomocaris, Doli- 
 chometopus, Anpocaris, Solenopleura, Eliipso- 
 cephalxbs , Arionellus, Conocoryphe, Olenus, Ace- 
 rocaris, Hydrocephalus, Paradoxides, Loncho- 
 cephalus, Dikelocephalus, Palceopyge. 
 
 See also Kept. 35th Meeting Brit. Assoc. Adv. 
 Sci., 1865, Trans, of Sec., p. 79 ; Geol. Mag., vol. 
 
 2, London, 1865, p. 468. 
 
 and Blanford (H. F. ) Palaeontology 
 
 of Nib, in the northern Himalayas. 
 Calcutta, 1865. 
 
 On some additional fossils from the 
 
 Lingula flags, with a note on the genus 
 Anopolenus , by Henry Hicks. 
 
 In Quart. Jour. Geol. Soc. London, vol. 21, 
 1865, p. 476. 
 
 Anopolenus, Conocoryphe, Microdiscus, Holo- 
 cephalina, Agnostus, Erinnus n. g. 
 
 On the fossils of North Wales. 
 
 In Mem. Geol. Survey Gt. Brit., vol. 3, Lon- 
 don, 1866, p. 239, 37 pis. 
 
 Dikelocephalus, Olenus, Parabolina, Conoco- 
 ryphe, Angelina, Homalonotus. Lichas, Trinu- 
 cleus, Dionide, Ampyx, Asaphus, Niobe, JEglina, 
 Cheirurus, Encrinurus, lllcenus, Agnostus, Psi- 
 locephalus, Beyrichia, Hymenocaris. 
 
 A monograph of British Trilobites. 
 
 Pt. 4. Pp. 177-216, pis. 25-30. 
 
 In Palaeont. Soc., vol. 20, 1867. 
 
 Ogygia, Barrandia, lllcenus, subgenera Oc- I 
 tillcenus, Panderia, Dysplanus, lllcenus, Ectil- | 
 Icenus, Hydrolcenus, Illcenopsis, and Bumastus. \ 
 Family Bronteidce. 
 
 A monograph of British Trilobites. 
 
 This work forms different parts of the Palae- ! 
 ont. Soc. London, volumes for 1862-’67, as sepa- 
 rately itemized in this connection. 
 
 On Saccocaris major. 
 
 In Kept. Proc. Geol. Poly tech. Soc. West Rid- 
 ing of Yorkshire (for 1867), vol. 4, 1868, p. 588. 
 
 and Hicks (Henry). On some fos- 
 sils from the Menevian group. 
 
 In Quart. Jour. Geol, Soc. London, vol. 25, 
 J869, p. 51, pis. 2, 3. 
 
 Salter (J. W.) — Continued. 
 
 Paradoxides, Plutonia n. g., Conocoryphe. 
 
 In a note on p. 52, Mr. J. W. Salter suggests 
 the new generic name of Plutonia, but leaves 
 the description for another article. 
 
 A species of this genus was afterwards de- 
 scribed and figured in the same journal, vol. 27, 
 1871, p. 299, pi. 15, figs. 1-8, under the name of 
 Plutonia sedgwicki Hicks. This large species 
 has affinities with the genera Paradoxides and 
 Anopolenus in the form of its glabella, but dif- 
 fers, according to Hicks, “in having the whole 
 surface covered with coarse tubercles or 
 spines.” The term Plutonia is objectionable, 
 inasmuch as it was used in 1864 for a genus of 
 the Mollusca. 
 
 Catalogue of the collection of Cam- 
 brian and Silurian fossils contained in 
 the Geological Museum of the Univer- 
 sity of Cambridge, 1873. 
 
 and Etheridge (R.) On the fossils 
 
 of North Wales. 
 
 In Geology of North W ales, with an appendix 
 on the fossils by J. W. Salter, revised and added 
 to by K. Etheridge ; Mem. Geol. Survey Gt. 
 Brit., vol. 3, London, 1881, 2d ed., 623 pp., 113 
 illustrations, 2 geol. maps, 26 plates of fossils. 
 
 Paradoxides, Plutonia, Anopolenus, Dikelo- 
 cephalus, Olenus, j ( Sphcerophthalmus ), Cono- 
 coryphe, Angelina, Arionellus, Phacops, Caly- 
 mene, Homalonotus , Lichas, Trinucleus, Ampyx, 
 Dionidce, JEglina, Asaphus, Ogygia , Barrandia, 
 Niobe, lllcenus, Illcenopsis, Cheirurus, Placo- 
 paria, Encrinurus, Cybele, Agnostus , Microdis- 
 cus, Carausia, Holocephalina, Nesuretus, Psilo- 
 cephalus, Hymenocaris, Lingulocaris, Ceratio- 
 caris, Entomis, Beyrichia, Leperditia. 
 
 Monograph of British Trilobites from 
 
 the Cambrian, Silurian, and Devonian 
 formations. Pt. 5. 
 
 Palaeont. Soc. London, vol. 37, 1883, pp. 215, 
 and index, 3 figs. 
 
 lllcenus bowmanni?, I. crassicauda, I. ( Bu- 
 mastus ) sp. ? 
 
 See Huxley (T. H.) and Salter (J. 
 
 W.). Also Salter (J. W.) and Sharpe 
 (D.). 
 
 Sars (M.) Ueber einige neue oder un- 
 vollstaudig bekannte Trilobiten. 
 
 In Isis (oder Encycl. Zeitung), Oken, 1833, 
 p. 33. 
 
 Scheuchzer ( J. J.) Specimen lithologim 
 Helvetia. Turici, 8vo, 1702. (*) 
 
 Metoorologia et Orytographia Hel- 
 vetica, oder Beschreibung der Luftge- 
 schichten, Steinen, Metallen, etc. Tu- 
 
 | rici, 1718. (*) 
 
VOGDES. J 
 
 LIST OF AUTHORS, 
 
 G5 
 
 Schlotheim (E. Fr. von). Beschreibuug 
 einer seltenen Trilobiten-Art. 
 
 In Taschenbuch fiir gesam. Mineral., Leon- 
 hard, 1810, pi. 1, figs. 1-6. 
 
 Trilobiten cornigerus Schloth. 
 
 Nachtrage zur Petrefactenkunde. 
 
 11. Gotba, 1823, pi. 22. 
 
 1. Trilobites blumenbachii, 2. T. tristani , 3. T. 
 variolatus , 4. T. macrophthalmus, 5. T. sulzeri, 
 
 6. T. hoffi, 7. T. cornigerus , 8. T. de buchii, 9. T. 
 hausmani , 10. T. schroet, 11. T. caudatus, 12. T. 
 laticauda, 13. T. guettardi, 14. T. desmarestii, 
 15. T. tessini, 16. T. spinulosus, 17. T. scara- 
 boides, 18. T. gibbosus, 19. T. laciniatus , 20. T. 
 sphcerocephalus, 21. T. pisiformis, 22. T. granu- 
 latu8, 23. T. punctatus, 24. T. mucronatus, 25. 
 
 T. bucephalus , 26. T. crassicauda, 27. T. tenta- 
 culatus, 28. T. problematicus, 29. T.bitumenosus. 
 
 Beschreibuug eiuiger abgebildeteu 
 
 Arten von Echinosphseriten und Tri- 
 lobiten. o 
 
 In Isis (oder Encycl. Zeitung), Oken, 1826, p. 
 309, pi. 1, figs. 8, 9 ; also F6russ., Bull., 1827, vol. 
 
 12, p. 406. 
 
 Tril. esmarcki , T. granum ( Agnostus ). 
 
 Schmid (E. E.) Die kleineren organi- 
 schen Formen des Zechsteinkalkes von 
 Setters in der Wetterau. 
 
 In Neues Jahrbuch fiir Mineral., 1867, p. 
 676, plate. 
 
 Cy there. 
 
 Schmidt ( Fr. ) Untersuckungen iiber 
 die silurische Formation von Ehstland, 
 Nord-Livland und Oesel. 
 
 In Archiv Naturk. Liv-, Ehst- u. Kurl., 
 Dorpat, vol. 2, 1858-59, pp. 443, 445, 448, 453, 
 461, 463. 
 
 Miscellanae Silurica. I. Ueber die 
 
 russischen silurischen Leperditien mit 
 Hinznziehung einiger Arten aus den 
 Nachbarlandern. 
 
 In M6ua. Acad. Imp. Sci. St.-P6tersbourg,vol. 
 21, No. 2, 1873, 1 pi. 
 
 Leperditia, Isochilina. 
 
 Einige Bemerkungen iiber die po- 
 
 dolisch-galizische Silurformation und 
 deren Petrefacten. St. Petersburg, 
 1875, 1 pi. 
 
 Proetus, CyphaspU, Phacops, Oalymene, En- 
 crinurus, Sphcerexochus, lllcenus ( Bumastus ), 
 Leperditia , Eurypterus, Pterygotus. 
 
 Revision der ost-baltischen siluri 
 
 schen Trilobiten, nebst geognostischer 
 Uebersicht des ost-baltischen Silurgo- 
 biets. 
 
 In M6m. Acad. Imp. Sci. St.-P6tersbourg, vol. 
 30, No. 1, 1881, 16 pis. 
 
 Phacopid®, genera, Phacopx. Acaste, Ptcrygo- | 
 metopus u. g., Ohasmops. Cheirurida 1 ., genera, ! 
 Cheirums, Cyrtometopus, tiphcercxochus, Pscu- | 
 
 Bull. G3 5 
 
 Schmidt (Fr.)— Continued. 
 
 dosphoerexochus n. g., Nieszkowskia n. g., Am- 
 phion, Diaphanometopus n. g., Encrinurid® 
 Cybele, Encrinurus. 
 
 and Jones (T. Rupert). On some 
 
 Silurian Leperditia. 
 
 In Annals Nat. Hist., 4th series, vol. 9, Lon- 
 don, 1882, p. 168. 
 
 Miscellanae Silurica. III. 1. Nach- 
 
 trag zur Monographie der russischen 
 silurischen Leperditien. 2. Die Crus- 
 taceenfauna der Eurypterenschichten 
 von Rootzikiill auf Oesel. 
 
 In M6m. Acad. Imp. Sci. St.-P6tersbourg,vol. 
 31, No. 5, 1883, 9 pis. 
 
 Leperditia, Bunodes, Pseudoniscus, Eurypte- 
 rus, Pterygotus , Geratocaris. 
 
 and Jones (T. Rupert). See Jones 
 
 (T. Rupert) and Schmidt (Fr.). 
 
 Ueber einige neue ostsibirische 
 
 Trilobiten und verwandte Thierformen. 
 
 In Bull. Acad. Sci. Imp. St.-P6tersbourg, vol. 
 30, No. 4, 1886, p. 502. 
 
 Agnostus, Phacops , Proetus, Oyphaspis, Eu- 
 rypterus. 
 
 Schrenk (G. A.) Uebersicht des obern- 
 silurischen Schichten-Systems Liv- und 
 Ehstlands, etc. 
 
 In Archiv Naturk. Liv-, Ehst- u. Kurl., 
 Dorpat, vol. 1854, pp. 35 and 86. 
 
 Leperditia. 
 
 Scouler (John). Description of a fossil 
 crustaceous animal. (*) 
 
 In Edinb. Jour. Nat. Geogr. Sci., Vol. 3, 1831, 
 p. 352, pi. 10. 
 
 The author describes in this article, under 
 the new generic name of Eidothea, certain frag- 
 ments of an Eurypterus. 
 
 Account of some fossil Crustacea 
 
 which occur in the coal formation 
 ( Argas ). 
 
 In Record of Geol. Sci. (Thomson’s), vol. 1, 
 1835, p. 136. 
 
 According to Capt. J. E. Portlock (Rept. 
 Geol. Londonderry, etc., 1843, p. 313), “ Dr. John 
 Scouler first noticed this remarkable Crusta- 
 cean found by him in the Carboniferous strata 
 of Paisley; and depending as a principal charac- 
 ter on the lateral caudal appendages, he pointed 
 out its analogy to the genera Cyclops and Apus; 
 and again, at the meeting of the British Associa- 
 tion at Glasgow, he described two species, one 
 of which, Argas tricornis, in all probability de- 
 pends on an illusive appearance produced by tho 
 overlapping of the crust of different individuals. 
 * * * I)r. John Scouler having subsequently al- 
 tered his view of the affinities of the genus, ho 
 now considers it a bi-valved Crustacean, dis- 
 tinguished by not being able to retract tho tail 
 within tho shell, and hence has named it Dilhy- 
 
66 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63. 
 
 Scouler (John)— Continued. 
 
 rocaris, or bivalved shrimp, abandoning the 
 original name as one already pre-occupied.” 
 
 TheRept. 10th Meeting Brit. Assoc. Adv. Sci., 
 1840, held at Glasgow, does not contain in the 
 index Dr. iScotiler’s name or that of the genus 
 Argos or Dithyrocaris. In the 5th Kept, of the 
 “Committee on the Fossil Phyllopoda of the Pa- 
 laeozoic Rocks,” 1887, the genus Dithyrocaris 
 Scouler is quoted on the authority of Captain 
 Portlock as follows : “ Dithyrocaris Scouler in 
 Portlock’s Geol. Report, Londonderry, etc., 
 1843,” p. 313. 
 
 Scudder (Samuel H.) Ehachura, a new 
 genus of fossil Crustacea. 
 
 In Proc. Boston Soc. Hat. Hist., vol. 19, 1878, 
 p. 296, pi. 9, figs. 3, 3 a. 
 
 In the 5th Rept. to the Brit. Assoc. Adv. 
 Sci., 1887, on the fossil Phyllopoda by the com- 
 mittee, consisting of Mr. R. Etheridge, Dr. H. 
 Woodward, and Prof. T. Rupert Jones this 
 new genus of S. H. Scudder is referred to as 
 probably of that of Dithyrocaris Scouler, 1843. 
 
 Shaler (N. S.) and Foerste (A. F.) Pre- 
 liminary description of North Attle- 
 borough fossils. 
 
 In Bull. t >Iu8. Comp. Zool. Harvard Coll., 
 vol. 16, Ho. 2, 1888, Geol. Series, vol. 2, 1888, p. 27, 
 2 pis. 
 
 Paradoxides, Ptychoparia, Microdiscus. 
 
 Sharpe (Daniel). On the geology of 
 the neighborhood of Oporto, including 
 the Silurian, coal, and slates of Val- 
 longo. 
 
 In Quart. Jour. Geol. Soc. London, vol. 5, 
 1849, p. 142.pl. 6. 
 
 Isotclus powissii Port., Illcenus lusitanicus 
 
 Sharpe. 
 
 Description of the new species of 
 
 Zoophyta and Mollusca. Appendix B 
 to an article on the Carboniferous and 
 Silurian formations of the neighbor- 
 hood of Bussaco, in Portugal, by C. 
 Ribeiro. 
 
 In Quart. Jour. Geol. Soc. London, vol. 9, 
 1853, p. 146. 
 
 Dithyrocaris? longicauda Sharpe. 
 
 Shumard (B. F.) Palaeontology. Crus- 
 tacea. 
 
 In 1st and 2d Ann. Repts. of the Geol. Survey 
 of Missouri (Swallow), 1855, pt. 2, p. 195, pi. B. 
 
 Proetus , Gyphaspis, Phillipsia, Dalmania , 
 Calymene, Acidaspis, Encrinurus, Cythere. 
 
 Notice of new fossils from the Per- 
 mian strata of New Mexico and Texas, 
 collected by Dr. George G. Shumard, 
 geologist of the U. S. Government ex- 
 pedition for obtaining water by means 
 of artesian wells along the 32d parallel, 
 
 Shumard (B. F.)— Continued, 
 under the direction of Capt. John Pope, 
 U. S. Corps of Top. Eng. 
 
 Trans. Acad. Sci. St. Louis, vol. 1, 1858, p. 290. 
 
 Phillipsia perannulata, pi. 11, fig. 10. 
 
 The Primordial zone of Texas, with 
 
 descriptions of new fossils. 
 
 In Am. Jour. Sci., 2d series, vol. 32, 1861, p. 
 213. 
 
 Dikelocephalus, Conocephalites, ArioneUus , 
 Agnostus. 
 
 Notice of some new and imperfectly 
 
 known fossils from the Primordial 
 zone (Potsdam sandstone and calcif- 
 erous sand group) of Wisconsin and 
 Missouri. 
 
 In Trans. Acad. Sci. St. Louis, vol. 2, 1863, p. 
 
 101 . 
 
 Dikelocephalus , Arionellus, Conocephalites, 
 Agnostus. 
 
 Descriptions of new Palaeozoic fos- 
 sils. 
 
 In Trans. Acad. Sci. St. Louis, vol. 2, 1863, p. 
 108. 
 
 Proetus proutii. 
 
 Sjogren (A.) Anteckningar om Oland, 
 ett bidrag till Sveriges geologi. 
 
 In Ofversigt K. Vet.-Akad. Forhandl. Stock- 
 holm, vol. 8, 1851, Ho. 2, p. 36. 
 
 Enumerates species of the following genera: 
 Pemopleurides , Paradoxides, Ellipsocephalus, 
 Olenus, Phacops, Calymene, H omalonotus, Li- 
 chas, Ampyx, Cheirurus, Asaphus, Illcenus, 
 Nileus, Battue, Cytherina. 
 
 Om nagra forsteningar i Olands 
 
 Kambriska lager. 
 
 In Geol. Foreningens Stockholm Forhandl., 
 vol. 1, Ho. 5, 1871, 1 pi. 
 
 Paradoxides, Ellipsocephalus , Conocoryphe, 
 Agnostus. 
 
 Sowerby (J. D. C.) Description of Ho- 
 malonotus knighti in Adam Sedgwick 
 and R. I. Murchison’s article on the 
 older formation on the right bank of 
 the Rhine, etc. 
 
 In Trans. Geol. Soc. London, 2d series, vol. 6, 
 1842, p. 275, figure, pi. 38, fig. 17. 
 
 Stainer (X.) Note sur un Trilobite nou- 
 veau. 
 
 In Annales Soc. G6ol. Belgique ; M6moires, 
 vol. 14, 1887. 
 
 Dechenella. 
 
 Steinhart (E. T. G.) Die bis jetat in 
 preuss. Geschieben gefundenen Trilo- 
 biten. 
 
 In Beitrage zur Hatur. Preuss., herausge- 
 geben von der phys. - okonomischen Gesell., 
 Konigsberg, 1874. 
 
VOGDES.} 
 
 LIST OF AUTHORS. 
 
 G7 
 
 Steinhart (E. T. G.) — Continued. 
 
 Harpes, Proetus, Cyphaspis, Phacops, C ha- 
 mops, Galymene, Dalmania, Licha, Ampyx , 
 Asaphus , A. ( Basilicus ), Illcenus , Nileus , jBw- 
 mastus, Acidaspis, Ceraurus, Sphcerexochus , 
 Zethus, Encrinurus, Aynostus. 
 
 Steininger (Jean). Observations sur les 
 fossiles du calcaire interm^diaire de 
 l’Eifel. 
 
 In M6m. Soc. G6ol. France, vol. 1, 1831, p. 331, 
 
 pL 21. 
 
 Galymene brongniarti, G. latreilii, G. schlot- 
 heimii, C. tristani, Proetus n. g., P. cuvieri, 
 Olenus punctatus, Asaphus mucronati, A.lati- 
 cauda. 
 
 Sternberg (Kasper Graf von). Ueber- 
 sicht der in Bohmen dermalen bekann- 
 ten Trilobiten. 
 
 In Yerhandl. mineral. Gesell. vaterlandisch. 
 Mus. Bohm., 1825, p. 69, pis. 2, 3; Isis (oder 
 Encycl. Zeitnng), Oken, vol. 7, 1827, p. 627. 
 
 Trilobites macrophthalmus, T. hausmanni, T. 
 sulzeri, T. hoffii, T. tessini. 
 
 Ueber die Gliederung und die Ftisse 
 
 der Trilobiten. 
 
 In Isis (oder Encycl. Zeitung), Oken, 1830, 
 pp. 516, 563, pi. 5, figs. 1-3. 
 
 Ueber bbhmische Trilobiten. 
 
 In Yerhandl. mineral. Gesell. vaterlandisch. 
 Mus. Bohm., 1833, p. 17. 
 
 Olenus longicaudatus, Trilobites spinosus, 
 Olenus pyramidalis, O. latus, Conoceph. costa- 
 tus, Trilobites sulzeri, T. zippii, Ellipsocephalus 
 ambigus, Trilobites hojji, Otarion diffractum, 
 Trilobites sternbergi, T. ungula, T. or natus. 
 
 Ueber die bohmischen Trilobiten mit 
 
 Beziehung auf die Arbeiten von Boeck 1 
 nnd Zenker dariiber. 
 
 In Neues Jahrbuch fur Mineral., 1835, p. 727. 
 
 Olertus longicaudatus, O. latus, Trilobites 
 minor, T. gracilus, T. sulzeri, T. hoffi, T. stern- 
 bergi, T. angula, T. ornatus, T. gibbosus, Otarion 
 diffractum. 
 
 Steschegloff. Treatise on the Trilobites 
 of Petersburg. (*) 
 
 In Jour, fur neue Entdeckungen in der 
 Phys , Chera., Natur., und Technologic, St. Pe- 
 tersburg, Jibs. 1, 2, 1827, pi. 8. (In Russian.) 
 
 Deucalion n. g. 
 
 Stock (Thomas). Note on the occur- 
 rence of Anthrapalcemon etheridgi B. N. 
 Peach, in the ironstones above the 
 sandstones at Craigleith Quarry, near 
 Edinburgh. 
 
 In Trans. Edinb. Geol. Soc., vol. 4, 1881, p. 97. 
 
 Note on the occurrence of the re- 
 mains of Decapod Crustaceans in the 
 
 Wardie shales. 
 
 Stock (Thomas) — Continued. 
 
 In Trans. Edinb. Geol. Soc., vol. 4, 1882, p. 
 219. 
 
 Palceocrangon, Anthrapalcemon. 
 
 Stoddart (W. W.) On Trilobites. 
 
 In Proc. Bristol Nat. Sei., vol. 1, 1866, p. 82. 
 
 Stokes (Charles). On a Trilobite from 
 Lake Huron. 
 
 In Trans. Geol. Soc. London, 2d series, vol. 
 1, 1822, p. 208, pi. 28. 
 
 Strauss-Durckheim (H.) Ueber Estlie - 
 via dahalacensis Riiffell, eine neue Gat- 
 tung aus der Familie der Daphniden. 
 
 In Mus. Senckenberg : anum, vol. 2, 1837, pp. 
 119-128, pis. 7, 7 b. 
 
 The name Estheria was originally proposed 
 by Dr. Ruffell for a species brought from Abys- 
 sinia; its description, with figures of typical 
 species, appeared in the above cited work. In 
 the same year Mr Audouin (Annales Soc. En- 
 tom., vol. 6) proposed that of Gyzicus for simi- 
 lar species, without a generic description. The 
 simultaneous publication of these two generic 
 names for the same genus lead Mr. Joly (An- 
 nales Sci. Nat., 2d series, vol. 17, 1842, p.293) to 
 propose that of Isaura. Estheria is now gene- 
 rally used by authors. 
 
 Symonds (W. S.) On a Phyllopod Crus- 
 tacean in the Upper Ludlow rock of 
 Ludlow. 
 
 In Kept. 25th Meeting Brit. Assoc. Adv. Sci., 
 1855, Trans, of Sec., p. 98. 
 
 Hymenocaris vermicauda. 
 
 On a new species of Eurgpterus from 
 
 the Old Red Sandstone of Hereford- 
 shire. 
 
 In Kept. 27th Meeting Brit. Assoc. Adv. Sci., 
 1857, Trans, of Sec., p. 93. 
 
 On a new species of Eurgptems from 
 
 the Old Red Sandstone of Hereford- 
 shire. 
 
 In Edinburgh New Philos. Jour., vol. 6, 1857, 
 p. 257. 
 
 Tate (George). Fame Islands. 
 
 In Proc. Berwickshire Nat. Club, vol. 3, No. 
 7, p. 222. 
 
 Griffithides farnensis. 
 
 Thomson (P. Wyvillo). Oil some spe- 
 cies of Acidaspis from the Lower Silu- 
 rian beds of the south of Scotland. 
 
 In Quart. Jour. Geol. Soc. London, vol. 13, 
 1857, p. 206, pi. 6. 
 
 Figures and descriptions illustra- 
 tive of organic remains. 
 
 In Geol. Survey United Kingdom, decade XI, 
 London, 1864, pi. 6. 
 
 Salter ia primes va Wyv. Thomson n. g. and 
 sp. 
 
68 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Tietze ( E. ) Ueber die devonischen 
 Schichten von Ebersdorf unweit Neu 
 rode in der Grafschaft Glatz. 
 
 In Geognostisch - palseont. Monographic, 
 Stuttgart, 1870, 2 pis. 
 
 Harpes , Proetus, Phacops, Cypridina. 
 
 Todd (J. E.) A description of some fos- 
 sil tracks from the Potsdam sandstone. 
 
 In Trans. Wisconsin Acad. Sci., vol. 5, 1882, 
 p. 276, 1 fig. 
 
 Tornquist ( S. L. ) Om lagerfoljden i 
 Dalarnes under-Siluris <a bildningar. 
 
 In Lunds TJniv. Arsskrift, vol. 3, 1867. 
 
 Berattelse om en geologisk resa 
 
 genom Skanes och Ostergotlands pa- 
 leozoiska trakter sommaren 1875, etc. 
 
 In Ofversigt Kongl. Svenska Yet. Akad. 
 Forhandl., 18:5, No. 10, p. 43. 
 
 Paradoxides, Olenus, Phacops, Calymene , 
 Asaphus, Illcenus , Trinucleus, Lichas , Agnos • 
 tus. 
 
 Undersokningar bfver Siljansomra- 
 
 dets Trilobitfauna. 
 
 In Svenska Geol. IJndersdkning, Stockholm, 
 series C, No. 66, 1884, 2 pis. 
 
 Harpes, Pemopleurides, Triarthrus, Proelus, 
 Gyphaspis , Arethusina, Isoielus, Phacops, Pha- 
 cops ( Pterygometopus ), Phacops ( Ghasmops ), 
 Calymene, Romalonotus, Lichas, Trinucleus, 
 Ampyx, Deiphon, Asaphus, Megalaspis, Niobe, 
 Acidaspis, Cheirurus, Sphcerexochus , Cyrtome- 
 topus, PseudosphcerexocMis , Nieszlcowskia , Sphce- 
 rexocoryphe, Pliomera, Encrinurus, Cybele, 
 Bronteus, Illcenus, Nileus, Agnostus. Telephus. 
 
 Torrubia (J.) Aparato para la historia 
 natural espanola. Yol. 1. Madrid, 
 1754, p. 83, par. 13, No. 96. 
 
 The Rev. Father Joseph Torrubia has the 
 merit of referring the Trilobites to the class 
 Crustacea. 
 
 Traquair (R. H.) Occurrence of Trilo- 
 bites in the Carboniferous limestone of 
 Fifeshire. (*) 
 
 In Proc. Royal Phys. Soc. Edinburgh, vol. 2, 
 1858-’61 , p. 253. 
 
 On the Grijffithides mucronatus Mc- 
 Coy. 
 
 In Jour. Royal Geol. Soc. Ireland, vol. 2, 1869, 
 p. 213, plate. 
 
 Trautschold (H.) Die Trilobiten als 
 Erstgeborene. 
 
 In Bull. Soc. Imp. des Naturalistes, Moscou, 
 1872, p. 297. 
 
 Die Kalkbruche von Mjatschkowa. 
 
 Eine Monographie des oberen Berg- 
 kalkes. 
 
 In M6m. Soc. Imp. des Naturalistes, Moscou, 
 vol. 13, 1874, p. 276. 
 
 Trautschold (H.)— Continued. 
 
 Phillipsia globiceps, P. grunswaldti, P.pustu • 
 lata. 
 
 Trenkner (M. W.) Paloeontolog. Novi- 
 taten vom nordwestl. Harze. Halle, 
 1367-’69, 8 pis. 
 
 Harpes, Gyphaspis, Bronteus, Entomis. 
 
 Tristan (J.) Sur un crustac6 renfermd 
 dans quelques schistes, notamment dans 
 ceux des environs de Nantes (d6pt. de 
 la Loire-Inf4rieure) et d’ Angers (ddpt. 
 de Maine-et-Loire). 
 
 In Jour. Mines, vol. 23, 1808, p. 2. 
 
 ( Calymene tristani Brong.) 
 
 Tromelin (G.) andLebesconte (P.) Ob- 
 servations sur les terrains primaires du 
 nord du d6pt. d’llle-et-Vilaine et de 
 quelques autres parties du massif bre- 
 ton. 
 
 In Bull. Soc. Geol. France, 3d series, vol. 4, 
 1875-76, p. 583. 
 
 Dalmanites, Calymene, Homalonotus, Trinu- 
 cleus. 
 
 Tschernyschew. Die Fauna des mittl. 
 und oberen Devon am Westabhange 
 des Urals. 
 
 In Mem. du Comit6 G6ol., vol. 3, No. 3, 1887, 
 p. 14. 
 
 Dechenella. 
 
 Tullberg (S. A.) Om ^ywosfws-arterna i 
 de Kambriska aflagringame vid Andra- 
 rum. 
 
 In Svenska Geol. Undersok., series C, No. 42, 
 1882, 2 pis. 
 
 Ulrich (E. O.) Description of some spe- 
 cies of fossils from the Cincinnati group. 
 
 In Jour. Cincinnati Soc. Nat. Hist., vol. 1, 
 1878-79, p. 92. 
 
 Trinucleus bellulus. 
 
 Description of a Trilobite from the 
 
 Niagara group of Indiana. 
 
 In Jour. Cincinnati Soc. Nat. Hist., vol. 2, 
 1879, p. 131, 3 figs. 
 
 Calymene nasuta. 
 
 Descriptions of new genera and spe- 
 cies from the Lower Silurian about Cin- 
 cinnati. 
 
 In Jour. Cincinnati Soc. Nat. Hist., vol. 2, 
 1879, p. 8, pi. 9. 
 
 Beyrichia, Leperditia. 
 
 Verneuil (Edouard). Sur les fossiles d6- 
 voniens des environs de Sabers dans les 
 montagnes de L6on. 
 
 In Bull. Soc. G6ol. France, 2d series, vol. 7, 
 1850, p. 155, pi. 3. 
 
 Cryphceus calliteles, Phacops lati/rons, 1 roma- 
 lonotus pradianus. 
 
VOGDES.] 
 
 LIST OF AUTHORS. 
 
 69 
 
 Verneuil (Rdouard) — Continued. 
 
 Geologic de la Russie d’Europe et 
 
 des montagnes de l’Oural, par R. I. 
 Murchison, Edouard de Verneuil et le 
 cointe Alex, de Keyserling. Vol. 2. 3 
 
 part. Palajontologie. Londres et Paris, 
 1845, 50 pis. 
 
 Calymene odini , C. fischeri, Asaphus expan- 
 sue, Phillipsia eichwaldi, P. ouralica n. s. 
 
 and Barrande (Joachim). Descrip- 
 tion des fossiles trou\6s dans les ter- 
 rains silurien et devonien d’Almaden 
 d'une partie de la Sierra Morena et des 
 montagnes de Tobide. 
 
 In Bull. Soc. G6ol. France, 2d series, vol. 12, 
 1854-’55, p. 904, pis. 23, 24. 
 
 Ellipsocephalus pradoanus, Calymene pul- 
 chra, C. tristani, C. arago, C. transienus, Homa- 
 lonotus rarus , H. brongniarti, Placoparia tour- 
 neminei, Dalmanites socialis, D. dujardini, D. 
 vetillarti, D. torrubice, D. phillipsi, D. downin- 
 gice, Lichas hispanica, Tiinucleus gold/ussi, 
 Cheirurus marianus, Asaphus nobilis, A. cianus, 
 A. glabratus, A. contractus , Illcenus hispanicus , 
 1. sanchezi, Ogygia. 
 
 Sur Fexistence de la faune pri- 
 
 mordiale dans la chalne Cantabrigue, 
 par M. C. de Prado, suivie de la de- 
 scription des fossiles par MM. de 
 Verneuil et Barrande. 
 
 InBulL Soc. G6oL France, 2d series, vol. 13, 
 1860, p. 5.6, pis. 6-8. 
 
 Paradoxides, Conocephalites, Arionellus, Ag- 
 nosias . 
 
 and d’Archiac. ( Vicomte .) Paldon- 
 
 tologie sur la faune d6vonienne des 
 rives du Bosphore. Liste des fossiles 
 recueillis par Abdullah-Bey. 
 
 In Comptes Rendus Acad. Sci., Paris, 1867, p. 
 1217. 
 
 Note sur les fossiles recueillis en 
 
 1863 par M. de Tchihatchef aux envi- 
 rons de Constantinople. 
 
 In Boll. Soc. G6oL France, vol. 21, 1864, p. 147. 
 Homalonotus, Cheirurus. 
 
 Verworm (M. ) Zur Entwicklungsge- 
 schichte der Beynchieu. 
 
 In Zeitscbr. Deutsch. geol. Gesell. Berlin, 
 vol. 39, 1887, p. 27. 
 
 Vine (G. R.) Notes on the distribution 
 of the Entomostraca in the Wenlock 
 shales. 
 
 In Proc. Yorkshire Geol. Polytechnic Soc., 1 
 vol. 9, pt. 3, 1887-88, p. 393. 
 
 Vitry (Abbdde). M&noire sur les fossiles 
 du Tournaisds et les purifications en 
 g6n6ral, relativement a lour utility 
 pour la vie civile. 
 
 Vitry (Abbd de) — Continued. 
 
 In M6m. Acad. Roy ale Sci., Bruxelles, vol. 3, 
 1780, p. 15, pi. 1, fig. 1 ( Phillipsia ) ; pi. 3, figs. 9-11. 
 Vogdes (A. W.) Notes on the genera 
 Acidaspis, Odontopleura, and Cerato- 
 cephala, etc. 
 
 In Proc. Acad. Nat. Sci., 1877, p. 138. 
 
 Short notes on the geology of Ca- 
 toosa County, Georgia. 
 
 In Am. Jour. Sci., 3d series, vol. 23, 1879, p. 
 475. 
 
 Calymene rostrata n. s. 
 
 Description of a new Crustacean 
 
 from the Upper Silurian of Georgia, 
 with remarks on Calymene elintoni. 
 
 In Proc. Acad. Nat. Sci. Phila., 1880, p. 176, 4 
 figs. 
 
 Calymene rostrata, C. elintoni. 
 
 Fig. 3, Calymene elintoni, has been referred 
 by A. F. Foerste (Bull. Den. Univ., vol. 2, 1887, 
 p. 95, pi. 8, figs. 12, 16) to Calymene vogdesi. 
 
 A new Trilobite. 
 
 In 12th Ann. Rept. Geol. Nat. Hist. Survey 
 Minnesota, 1884, p. 8. 
 
 Bathyurus stonemani n. s. 
 
 Description of a new Crustacean 
 
 from the Clinton group of Georgia, with 
 remarks upon others. New York City, 
 1886, 5 pp., 4 figs. 
 
 Encrinurus americanus n. s., Calymene ros- 
 trata, and C. elintoni. 
 
 The genera and species of North 
 
 American Carboniferous Trilobites. 
 
 In Annals New York Acad. Sci., vol. 4, 1887, 
 p. 69, 2 pis. 
 
 Proetus, Phillipsia, Griffithides, Brachymeto- 
 pu8. 
 
 Description of two new species of 
 
 Carboniferous Trilobites. 
 
 In Trans. New York Acad. Sci., vol. 7, 1888, 
 p. 247, 1 wood-cut. 
 
 Phillipsia, Griffithides ? 
 
 Volborth (A.) Ueber einige russische 
 Trilobiten. 
 
 In Yerhandl. tubs. k. mineral. Gesell. zu St. 
 Petersburg, 1847, p. 1, pi. 1. 
 
 Tho author redescribed the genus Zethus 
 Pander and its type Zethus verrucosus, placing 
 Cybele bellatulus Eichw. under the same genus. 
 
 Ueber das Prioritiitsrecht der Trilo • 
 
 biten-Gattung Zethus Pander gegen die 
 Gattuug Cryptonymu8 Eichwald. 
 
 In Bull. Physico-Math. Acad. Sci., St.-P6ters- 
 bourg, 1854, p. 251. 
 
 Ueber die Bewegungs-Organe der 
 
 Trilobiten. Folgendes mit. 
 
 In Verhaudl. russ. k. mineral. Gesellsch.zn 
 St. Petersburg, 1857— ’58, p. 168. 
 
70 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 Volborth (A.)— Continued. 
 
 Ueber die Crotaluren und Remopleu- 
 
 riden, ein Beitrag zur Kenntniss der 
 russischen Trilobiten. 
 
 In Yerhandl. rass. k. mineral. Gesell. zu St. 
 Petersburg, 1857-58, p. 126, pi. 13. 
 
 Crotalurus n. g., Remopleurides. 
 
 Ueber die mit glatten Rumpfglie- 
 
 dern versehenen russischen Trilobiten, 
 nebst einem Anhange liber Bewegungs- 
 organe und fiber das Herz derselben. 
 
 In M6m. Acad. Imp. Sci. St.-P6tersbourg, 
 vol. 6, No. 2, 1863, 48 pp., 4 pis. 
 
 lllcenus, Dysplanus, Panderia n. g., Nileus, 
 Bumastus. 
 
 Ueber einige neue ehstlandische 
 
 Illsenen . 
 
 In M6tn. Acad. Imp. Sci. St.-P6tersbourg, 
 vol. 8, No. 9, 1864, 2 pis. 
 
 Ueber Herrn von Eicliwald’s Beitrag 
 
 zur naheren Kenntniss derlllaenen, etc. 
 
 In Bull. Soc. Imp. des Naturalistes, Moscou, 
 1866, No. 1, p. 77. 
 
 Wahlenberg (Geo.) Petrificata telluris 
 Suecana!' Upsaliae, 1818. 
 
 Tbis work was published and distributed in 
 1818 as a separate article, in advance of the 
 Nova Acta Reg. Soc. Sci., vol. 8, 1821. 
 
 Petrificata telluris Suecana exami- 
 
 nata a Georgio Wahlenberg. 
 
 In Nova Acta Reg. Soc. Sci., Upsal., vol. 8, 
 1821, pp. 1-116, pis. 1-4. 
 
 Entomostracites expansus Linn., E. crassicau- 
 da n. s., E. laticauda n. s., E. caudatus Brim., E. 
 granulatus n. s., E- tuberculatus Brim., E.punc- 
 tatus Brum, E. laciniatus n. s., E. paradozissi- 
 mus Linn. ( Paradoxides tessini), E. bucephalus 
 (hypostoma of P. tessini ), E. spinulosa n. s., E. 
 gibbosus n. s., E. scaraboeoides n. s., E. pisi- 
 f or mis Linn. 
 
 Additamenta qusedam ad petrificata 
 
 telluris Suecana. 
 
 In Nova Acta Reg. Soc. Sci., Upsal., vol. 8, 
 1821, pp. 293-296, pi. 7. 
 
 Entomostracites crassicauda, E. expansus , E. 
 tuberculatus , E. caudatus , E. laticauda. 
 
 Entomostracites crassicauda , pi. 7, fig. 5, has 
 been referred by G. Holm. (De Svenska Ar- 
 terna Trilobitslagetet lllcenus, 1882, p. 55) to 
 lllcenus esmarkii Sclilotheim. 
 
 Walch (J. E. T.) Des Trilobites dans 
 le rbgne des purifications, ou de la 
 conque rid6e a trois lobes (concha 
 triloba rugosa). Recueil des monu- 
 meus des catastrophes que le globe de 
 la terre a essui6es, contenaut despfitri- 
 fications. (Knorr, G. W.) Vol. 3. Nu- 
 remberg, 1775, p. 105. 
 
 Walch (J. E. T.) — Continued. 
 
 See also voL 2, 1768, section 1, p. 81 ; vol. 3, 
 1775, pp. 184, 185, 186, 193 ; suppl. pis. 8, 9 a, 9 b, 
 9 c, 9 e, 9 f. German and French editions. 
 
 This author gives the name of Trilobite to 
 the family, a designation which has been used 
 by all subsequent authors, with the exceptions 
 of J. W. Dalman and C. S. Rafinesque. 
 
 Walcott (C. D.) Description of a new 
 species of Trilobite [from Trenton Falls, 
 New York.] 
 
 In Cincinnati Quart. Jour. Sci., vol. 2, 1875, p. 
 273, 2 figs. 
 
 Sphcerocoryphe robustus. 
 
 New species of Trilobite from the 
 
 Trenton limestone at Trenton Falls, 
 N. Y. 
 
 In Cincinnati Quart. Jour. Sci., vol. 2, 1875, p. 
 347, wood-cuts. 
 
 Remopleurides striatulus. 
 
 Notes on Ceraurus pleurexanthemus 
 
 Green. 
 
 In Annals Lyceum Nat. Hist., New York, 
 vol. 11, 1876, p. 155, pi. 11. 
 
 Preliminary notice of the discovery 
 
 of the remains of the natatory and 
 branchial appendages of Tiilobites. 
 
 In 28th Rept. New York State Mus. Nat. 
 Hist., 1875, p. 89. 
 
 Description of new species of fossils 
 
 from the Trenton limestone. 
 
 In 28th Rept. New York State Mus. Nat. 
 Hist., 1875, p. 93. 
 
 Bathyurus, Asaphus. 
 
 Notes on some sections of Trilobites 
 
 from the Trenton limestone. 
 
 In 31st Rept. New York State Mus. Nat. 
 Hist., 1879, p. 61. Advanced sheets published 
 September 20, 1877, 1 pi. 
 
 Notes upon the legs of Trilobites. 
 
 In 31st Rept. New York State Mus. Nat. 
 Hist., 1879, p. 64. 
 
 Notes upon the eggs of the Trilobites. 
 
 In 31st Rept. New York State Mus. Nat. 
 Hist., 1879, p. 66. Advanced sheets published 
 September 20, 1877. 
 
 Descriptions of new species of fos- 
 sils from the Chazy and Trenton lime- 
 stones. 
 
 In 31st Rept. New York State Mus. Nat. 
 Hist., 1879, p. 69. Advanced sheets published 
 September 20, 1877. 
 
 Arionellus, Dcdmanites , Asaphus, Addaspis, 
 Ceraurus, Encrinurus, lllcenus. 
 
 The Utica slate and related forma- 
 tions of the same geological horizon. 
 
 In Trans. Albany Inst., vol. 10, 1879, p. 2, 
 pis. 1, 2. 
 
V0GDES. J 
 
 LIST OF AUTHORS. 
 
 71 
 
 Walcott (C.D.) — Continued. 
 
 Metamorphoses of Triarthrus becJci. 
 
 Triarthrus becki and JBeyriehia Cincinnati- 
 ensis. 
 
 Description of new species of fossils 
 
 from the Carboniferous formation. 
 
 In 32d Rept. New York State Cab. Nat. Hist., 
 1879, p. 129. Pamphlet published in advance of 
 the report 
 
 Conocephalites, Ptychaspis, Bathyurus. 
 
 The Trilobite, new and old evidence 
 
 relating to its organization. 
 
 In Mus. Comp. Zool. Harvard Coll., vol. 8, 
 1881, p. 191, 6 pis. 
 
 Description of a new genus of the 
 
 order Eurypterus from the Utica slate. 
 
 In Am. Jour. Sci., 3d series, vol. 23, 1882, p. 
 213, figures. 
 
 Echinognathus n. g. 
 
 Description of new species of fossils 
 
 from the Trenton group, New York. 
 
 In 35th Kept. Hew York State Cab. Hat. 
 Hist., 1883, p. 206, 1 pi. 
 
 Beyrichia, Leper ditia (Tsochilina ) . 
 
 Author’s edition, October 15, 1883, 8 pp., 1 pi. 
 
 Injury sustained by the eye of a 
 
 Trilobite at the time of moulting of the 
 shell. 
 
 In Annals Hat. Hist , 5th series, vol. 13, Lon- 
 don, 1884, p. 69. 
 
 On the locomotory appendages of 
 
 Trilobites. 
 
 In Science, vol. 3, 1884, p. 279, 3 figs. 
 
 Asaphus megistos, Calymene senaria. 
 
 Palaeontology of the Eureka district. 
 
 In Mon. H. S. Geol. Survey, vol. 8, 1884, 24 pis. 
 
 JHcellocephalus, Olenellus, Ptychoparia, P. 
 
 ( Solenopleura ), P. (Pterocephalus) , Anomocare, 
 Bathyurus , Chariocephalus, Ptychaspis , Agrau- 
 los, Proetus, Cyphaspis, Arethusina, Phillipsia, 
 Grifjithides, Phacops, Dalmanites, Trinucleus , 
 Asaphus, Symphysurus , Ogygia?, Barrandia? , 
 lllcenurus, Ceraurus, Amphion, Illcenus, Agnos- 
 tus, Leperditia, Beyrichia , Primitia, Plumulites. 
 
 On the Cambrian faunas of North 
 
 America. Preliminary studies. 
 
 In Bull. H. S. Geol. Survey, No. 10, 1884, 
 10 pis. 
 
 Paradoxides, Conocoryphe, Harttia n. g., Pty- 
 choparia, Agno8tu8, Microdiscus, Agraulos, Pro- 
 
 tocaris n. g. 
 
 Palaeozoic notes : New genus of Cam- 
 brian Trilobites, Mesonacis. 
 
 In Am. Jour. Sci., 3d series, vol. 29, 1885, p. 
 328, figures. 
 
 Describes a new genus, Mesonacis, and sub- 
 stitutes the generic name Bailiella of Matthew 
 for the subgenus & ' alter m, proposed by him j 
 (Bull. U. S. Geol. Survty, Ho. 10, lt84). 
 
 Walcott (C. D.) — Continued. 
 
 Second contribution to the studies 
 
 on the Cambrian fauna of North Amer- 
 ica. 
 
 In Bull. U. S. Geol. Survey, Ho. 30, 1886. 
 
 Figures and descriptions of species of the fol- 
 lowing genera are given, viz : Paradoxides , Ba- 
 thynotus, Mesonacis, Olenellus, Olenoides, Oryc- 
 tocephalus n. g , Ptychoparia, Solenopleura, 
 Anomocare, Grepicephalus, Dorypyge, Asaphis- 
 cus, Bathyuriscus, Agnostus , Microdiscus, Proty- 
 pus n. g., Protocaris, Leperditia. 
 
 Fauna of the upper Taconic of Em- 
 mons, in Washington County, New 
 York, with one plate. 
 
 In Am. Jour. Sci., 3d series, vol. 34, 1887, p. 
 187. 
 
 Solenopleura ?, Ptychoparia ?, Microdiscus, 
 Olenoides, Conocoryphe, Aristozoe, Leperditia. 
 
 Cambrian fossils from Mount Ste- 
 phens, North West Territory of Canada. 
 
 Am. Jour. Sci., 3d series, vol. 36, 1888, p. 161. 
 
 Ptychoparia, Agnostus, Bathyuriscus, Olenoi- 
 des, Zacanthoides n. g. 
 
 Stratigraphic position of the Olenel- 
 lus fauna in North America and Eu- 
 rope. 
 
 Am. Jour. Sci., 3d series, vol. 37, 1889, p. 374. 
 
 Leperditia, Aristozoa, Protocaris, Agnostus , 
 Microdiscus, Olenellus, Paradoxides , Olenoides, 
 Zacanthoides, Bathynotus, Avalonian, g., Cono- 
 coryphe, Ptychoparia, Agraulos, Grepicephalus, 
 Oryctocephalus, Anomocare, Protypus, Soleno- 
 pleura. 
 
 Waldschmidt (E.) Ueber die devoni- 
 schen Schichten der Gegend von Wild- 
 
 ungen. 
 
 In Zeitschr. Deutsch. geol. Gesell., vol. 37, 
 1885, p. 906, pis. 37-40. 
 
 Phacops, Bronteus, Cypridina. 
 
 Warder (John A.) New Trilobites. 
 
 In Am. Jour. Sci., 1st series, vol. 34, 1838, p. 
 377. 
 
 Geratocephala n. g. 
 
 This article on the new genus Geratocephala 
 was read before the Western Academy of Sci- 
 ence, May 25, 1838. 
 
 Washburn (W. T.) The geology of the 
 Bosphorus. 
 
 In Am. Jour. Sci., 3d series, vol. 6, 1873, p. 186. 
 
 Hot descriptive ; contains important notes on 
 fossil Crustacea. 
 
 Weitenweber (W. R.) Systematisches 
 Verzeichniss der bohmischen Trilobiten 
 in der Sammlung des Dr. Zeidler. 
 
 In Lotos, vol. 7, 1847, pp. 5-42. 
 
 Wetherby (A. G.) Description of a new 
 family and genus of Lower Silurian 
 Crustacea. 
 
I BULL. 63. 
 
 72 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Wetherby (A. G.) — Continued. 
 
 In Jour. Cincinnati Soc. Nat. Hist., vol. 1, 
 1878-79, p. 162, figure, vol. 2, pi. 7, figs. 1, 1 a^g. 
 Enoploura balanoides. 
 
 White (C. A.) and St. John (O. H.)— 
 Continued. 
 
 Calymene senaria, Cyphaspis christyi, Phil- 
 lipsia bufo. 
 
 Description of new fossils from the 
 
 Lower Silurian and Subcarboniferous 
 rocks of Ohio and Kentucky. 
 
 In Jour. Cincinnati Soc. Nat. Hist., vol. 4, 1 
 1881, p. 77. 
 
 Proetus, Isochilina. 
 
 White (C. A.) and St. John (O. H.) Pre- 
 liminary notice of new genera and 
 species of fossils. Iowa City, May 8, j 
 1867, 3 pp. 
 
 Beyrichia lithof actor, B. lithof actor var. velata, j 
 Oythere simplex. 
 
 Of this small pamphlet only fifty copies were 
 published by the Iowa State Geological Sur- j 
 vey. Republished in Trans. Chicago Acad, j 
 Sci., vol. 1, 1867. 
 
 Description of new subcarbon- ] 
 
 iferous and Coal-Measure fossils col- 
 lected upon the geological survey of 
 Iowa, together with a notice of new 
 generic characters observed in two 
 species of Brachiopods. 
 
 In Trans. Chicago Acad. Sci., vol. 1, pt. 1, I 
 1867, p. 115, 2 figs. 
 
 Beyrichia petrifactor, B. petrifactor var. 
 velata, B. foetoidea, Cythere simplex. 
 
 In this article the authors give the new 
 names of Beyrichia petrifactor to the species 
 described in the preliminary notice as B. litho- j 
 factor, and also change the name of B. litho- I 
 factor var. velata to that of Beyrichia petrifactor j 
 var. velata. 
 
 Preliminary report upon inverte- 
 brate fossils collected by the expedi- 
 tions of 1871, 1872, and 1873, with de- i 
 scriptions of new species. 
 
 In Geog. and Geol. Expl. Surveys West 100th j 
 Meridian, Washington, 1874. 
 
 Olenellus, Dicellocephalus, Megalaspis, Ag- 
 nostus, Leperditia. 
 
 Report upon the invertebrate fossils 
 
 collected in portions of Nevada, Utah, 
 Colorado, New Mexico, and Arizona, by 
 parties of the expeditions of 1871, 1872, 
 1873, and 1874. 
 
 In Geographical Surveys West 100th Meri- 
 dian, Palaeontology, vol. 4, 1877, pt. 1, pp. 1-219, 
 pis. 1-21. 
 
 Olenellus, Dicellocephalus , Asaphiscus, Cono- 
 coryphe ( Ptychoparia ), Megalaspis, Agnostus, 
 Leperditia. 
 
 Palaeontology : Fossils of the Indiana 
 
 rocks. 
 
 In 2d Ann. Rept. Dept. Statistics and Ge- | 
 ology, Indiana, 1880, pp. 471-522, pis. 1-11. 
 
 The fossils of the Indiana rocks. 
 
 No. 3. 
 
 In 13th Ann. Rept. Dept. Geol. and Nat. Hist. 
 Indiana, 1883, pt. 2, pp. 107-180, pis. 23-39. 
 
 Phillipsia (Griffithides?) scitala, P. ( G . ?) san- 
 gamonensis, Eurypterus ( Anthraconetes ) mazo- 
 nensis, Anthrapalcemon gracilis, Acanthotelson 
 stimpsoni, A. eveni , Palceocaris typus, Dithyro- 
 caris carbonarius, Leaia tricarinata, Euproops 
 dance, E. colletti. 
 
 Whiteaves (J. F. ) Palfeozoic fossils. 
 Yol. 3, pt. 1, 1884. 
 
 In Geol. and Nat. Hist. Survey Canada, 1884, 
 8 pis. 
 
 Eurypterus boylei. 
 
 Contributions to Canadian palaeon- 
 tology. Yol. 1. 
 
 In Geol. and Nat. Hist. Survey Canada, 1888. 
 
 In the author’s list of fossils from the Hamil- 
 ton formation of Ontario the following Crus- 
 tacea are included: Phacops bufo , Dalmanites 
 helena, D. boothii, and Cythere ? ( Beyrichia ) 
 punctulifera. 
 
 . See Matthew (G. F.) Illustra- 
 tions of the fauna of the St. John 
 group. No. 3. 
 
 In Trans. Royal Soc. Canada, vol. 3, 1885, 
 p. 76. 
 
 Solenopleura acadia Whiteaves. 
 
 Whitfield (R. P.) Description of new 
 species of fossils. 
 
 In Rept. Reconnoissance from Carrol, Mon- 
 tana Territory, on the Upper Missouri, to the 
 Yellowstone National Park and return, Lud- 
 low’s report, Washington, 1876. 
 
 Crepicephalus ( Loganellus ) montanensis, 
 Arionellus tripunctatus. 
 
 See, also, Rept. Chief Eng. U. S. A., 1876, 
 Appendix NN. 
 
 Preliminary descriptions of new 
 
 species of fossils from the lower geo- 
 logical formation of Wisconsin. 
 
 In Ann. Rept. Geol. Survey Wisconsin, 1877, 
 pp. 50-89. 
 
 Dicellocephalus, ConocephaXites, Ptychaspis, 
 Crepicephalus, Agraulus ( Bathyurusf ), Arionel- 
 lus, Ellipsocephdlus, Illcenurus, Bronteus. 
 
 Preliminary report on the palaeon- 
 tology of the Black Hills, containing 
 descriptions of new species of fossils 
 from the Potsdam, Jurassic, and Creta- 
 ceous formations of the Black Hills of 
 Dakota. 
 
 In U. S. Geol. Survey Rocky Mountain Re- 
 gion, Washington, 1877. 
 
 Crepicephalus (Loganellus) centralis , C. (Lo- 
 ganellus) planus. 
 
VOGDES.] 
 
 LIST OF AUTHORS. 
 
 73 
 
 Whitfield (R. P. )— Continued. 
 
 Description of new species of fossils 
 
 from the Palaeozoic formations of Wis- 
 consin. 
 
 In Ann. Rept. Geol. Survey Wisconsin, 1879, 
 • pp. 44-71. 
 
 DiceUocephalus, Orepicephalus ? , Ptychaspis, 
 Aglaspis, Conocephalites ? , Conocephalites (Pty- 
 chaspis ?), Asaphus, Illcenus. 
 
 New forms of' fossil Crustaceans 
 
 from the Upper Devonian rocks of 
 Ohio, with descriptions of new genera 
 and species. 
 
 In Am. Jour. Sci., 3d series, vol. 19, 1880, p. 33. 
 
 Echinocaris n. g., Palceopalcemon n. g. 
 
 A plate and explanation accompany the 
 author’s edition. 
 
 Palaeontology of the Black Hills of 
 
 Dakota. 
 
 In U. S. Geog. and Geol. Survey Rocky 
 Mountain Region. Rept. Geol. and Resources 
 of the Black Hills of Dakota, with atlas ; by 
 Henry Newton and Walter Jenney, Washing- 
 ton, 1880, p. 325, pi. 2. 
 
 Orepicephalus planus, O. centralis. 
 
 Palaeontology. 
 
 In GeoL Wisconsin, vol. 4, 1882, pt. 3, pp. 163- 
 363, pis. 1-27. 
 
 DikeUocephalus, Conocephalites , O. ( Ptychas- 
 pis ?), Ellipsocephalu8, Orepicephalus, Ptychas- 
 pis, Arionellus, A. ( Agraulos ), Agraulos (Bathy- 
 urus?), Aglaspis, I llcenur us, Asaphus, Illcenus, 
 Sphcerexochus, Phacops, Bronteus, Leperditia. 
 
 Description of new species of fossils 
 
 from Ohio, with remarks on some of the 
 geological formations in which they 
 occur. 
 
 In Annals New York Acad. Sci., vol. 2, Nos. 
 7, 8, 1882, p. 193. 
 
 Eurypterus, Leperditia, Plumulites. 
 
 . On the fauna of the Lower Carbonif- 
 
 erous limestones of Spergen Hill, Indi- 
 ana, with a revision of the descriptions 
 of its fossils heretofore published, and 
 illustrations of the species from the 
 original type series. 
 
 In Ball. Am. Mus. Nat. Hist. New York, vol. 
 1, No. 3, 1882, pi. 9. 
 
 Leperditia carbonaria Hall, Oytherellina glan- 
 della n. s. 
 
 Plates republished in 12th Rept. Geol. Nat. 
 Hist. Indiana, 1882. 
 
 List of Wisconsin fossils. 
 
 In GeoL Wisconsin, vol. 1, 1883, p. 362; also 
 illustrations of typical fossils of the Wisconsin 
 
 formations. 
 
 Notice of some new species of Pri- 
 mordial fossils in the collection of the 
 
 Whitfield (R. P.) — Continued. 
 
 Museum, and corrections of previously 
 described species. 
 
 In Bull. Am. Mus. Nat. Hist., New York, vol. 
 1, No. 5, 1884, p. 139, pis. 14, 15. 
 
 DikeUocephalus, Olenellus, Arionellus, Oono- 
 cephalites , Angelina. 
 
 Notice of a very large species of 
 
 Homalonotus from the Oriskany sand- 
 stone formation. 
 
 In Bull. Am. Mus. Nat. Hist., New York, vol. 
 1, No. 6, 1885, p. 193, pi. 22. 
 
 Homalonotus major Whitfield. 
 
 Notice of geological investigations 
 
 along the eastern shore of Lake Cham- 
 plain, conducted by Prof. H. M. Seely 
 and Prest. Ezra Brainerd, of Middle- 
 bury College, with descriptions of the 
 new fossils discovered. 
 
 In Bull. Am. Mus. Nat. Hist., New York,, vol. 
 
 1, No. 8, 1886, p. 293. 
 
 Saof lamottensis n. s., Lichas champlainensis 
 n. 8., Asaphus canalis Conrad. 
 
 Observations on some imperfectly 
 
 known fossils from the calciferous 
 sandrock of Lake Champlain, and de- 
 scriptions of several new forms. 
 
 InBull. Am. Mus. Nat. Hist., New York, vol. 
 
 2, No. 2, 1889, p. 41, 13 pis. 
 
 Primitia gregaria, P. ? cristata, P. seelyi, 
 Bathyurus conicus, B. seelyi. 
 
 Additional notes on Asaphus canalis 
 
 Conrad. 
 
 In Bull. Am. Mus. Nat. Hist., New York, vol. 
 2, No. 2, 1889, p. 64, pis. 11, 12. 
 
 Description of a new form of fossil, 
 
 Balanoid Cirripede, from the Marcellus 
 shale of New York. 
 
 In Bull. Am. Mus. Nat. Hist., New York, vol. 
 2, No. 2, 1889, p. 66. 
 
 Protobalanus n. g., P. hamiltonensis, pi. 13, 
 fig. 22. 
 
 See Hall (James) and Whitfield 
 
 (R.P.). 
 
 Wigand (Georg von). Ueber die Trilo- 
 biten der silurischen Geschiebe in 
 Mecklenburg. 
 
 In Zeitschr. Deutsch. geol. Ges., vol. 40, 1888, 
 p. 39, pis. 6-10. 
 
 Phacops, Lichas, L. (Hoplolichas), Illcenus, 
 Cheirurm, 0. (Oyrtometopus), O. ( Pseudosphce - 
 rexochus), O. (Nieszkowskia ) , Sphcerexochus, 
 Amphion, Cybele, Encrinurus, Acidaspis. 
 
 Wiik (F. G.) Om fossilierna i Alands 
 silur-kalksten jemfdrda med de i 
 Sverige och Estland fdrekommande. (*) 
 
 In Bidrag till Kannedom af Finlands Natur 
 och Folk, pt. 35, Helsingfors, 1881. 
 
74 
 
 A BIBLIOGRAPHY OP PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Wilckens (C. F.) Sendschreiben, worm 
 wahrscheinlich dargethan wird, dass die 
 Conchilioligisten eben keine Ursache 
 mebr baben, das Petrefact, welcbes 
 bisber unter der Benenmmg eines Uon- 
 chitce trilobi ragosi bekannt geworden 
 ist, als einen Tbeil ihrer Wissenscbaft 
 anzusehen. (*) 
 
 In Stralsundisches Mag., vol. 1, 1768, p. 267. 
 
 Nachricht von seltenen Versteine- 
 
 rungen, vornemlicb des Thier-Reiches, 
 welcbe bisber nocb nicht genau genug 
 bescbieben und erklart worden. Mit 
 Kupfern, in drei Sendsebreiben an seine 
 Gonner und Freunde. Berlin und 
 Stralsund, 1769, pi. 8. (*) 
 
 Williams (EL S.) On the occurrence of 
 Proetus longicauda Hall in Madison 
 County, Kansas. 
 
 In Am. Jour. Sci., 3d series, vol. 21, 1881, p. 
 
 156. 
 
 Notice of a new Limuloid Crustacean 
 
 from the Devonian. 
 
 In Amt Jour. Sci., 3d series, vol. 30, 1885, p. 45, 
 3 figs. 
 
 Prestwichia eriensis n. s. 
 
 This species was used by A. S. Packard 
 (Mem. Nat. Acad. Sci., vol. 3, 1888, p. 150) for the 
 type of bis new genus, Protolimulus. 
 
 Notice of a new Limuloid Crustacean 
 
 from the Devonian formation of Erie 
 County, Pennsylvania. 
 
 In Nature, vol. 32, London, 1885, p. 350. 
 
 Prestwichia eriensis. 
 
 Winchell (Alexander). Descriptions of 
 fossils from the Marshall and Huron 
 groups of Michigan. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 14, 1862, p. 
 405. 
 
 Oythere crassimarginata. 
 
 Description of fossils from the 
 
 yellow sandstone lying beneath the 
 Burlington limestone at Burlington, 
 Iowa. 
 
 In Proc. Acad. Nat. Sci. Phila., vol. 15, 1863, 
 
 p. 2. 
 
 Phillip8ia insignis, P. meramecensis. 
 
 Notice of a small collection of fossils 
 
 from the Potsdam sandstone of Wis- 
 consin and Lake (Superior sandstone of 
 Michigan. 
 
 In Am. Jour. Sci., 2d series, vol. 37, 1864, p. 
 226. 
 
 Dicellocephalus, Ptychaspis. 
 
 Description of new species of fossils 
 
 from the Marshall group of Michigan 
 
 Winchell (Alexander) — Continued, 
 and its supposed equivalent in other 
 States; with notes on some fossils of 
 the same age previously described. 
 
 In Proc. Acad. Nat. Sci. Pbila., vol. 17, 1865, 
 p. 109. . 
 
 Phillipsia rockfordensis , P. doris (Hall) Win- 
 chell. 
 
 and Marcy (O.) Enumeration of 
 
 the fossils collected in the Niagara 
 limestone at Chicago, 111. ; with de- 
 scriptions of some new species. 
 
 In Mem. Boston Soc. Nat. Hist., vol. 1, 1866, p. 
 
 81, pis. 2, 3. 
 
 Lichas, Addaspis, Bronteus, Illcenus. 
 
 Winchell (N. H.) Fossils from the red 
 quartzite at Pipestone. 
 
 In 13th Kept. Geol. Nat. Hist. Survey Minne- 
 sota, 1884, p. 65, plate. 
 
 Paradoxides barberi. 
 
 Woltersdorf (J. L.) Systema minerale. 
 Berlin, 1748, p. 42. 
 
 The author classes the Trilobites with the 
 Mollusca, calling them “Conchites trilobus.” 
 
 Woodward (Henry). On a nearly per- 
 fect specimen of Eurypterus lanceolatus 
 (Salter) from the Upper Ludlow rocks 
 at Lesmahagow, etc. 
 
 In Geol. Mag., vol. 1, London, 1864, p. 107, pi. 5. 
 
 On the Eurypteridcv and Xiphosura. 
 
 In Kept. 34th Meeting Brit. Assoc. Adv. Sci.,' 
 
 1864, Sec. C; Geol. Mag., vol. 1, London, p. 239. 
 Eurypterus , Pterygotus, Slimonia, Stylo nu~ 
 
 rus , Eemiaspis. 
 
 Descriptions of some new Palaeozoic 
 
 Crustacea. 
 
 In Geol. Mag., vol. 1, London, 1864, p. 196, pi. 
 
 10, wood-cuts. - 
 
 Eurypterus, Pterygotus, Stylonurus. 
 
 On some Crustacean teeth from the 
 
 Carboniferous and Upper Ludlow rocks 
 of Scotland. 
 
 In Geol. Mag., vol. 2, London, 1865, p. 401, 
 pi. 11. 
 
 Ceratiocaris, Dithyrocaris. 
 
 On some new species of Crustacea 
 
 belonging to the order Eurypteridce. 
 
 In Geol. Mag., vol. 2, London, 1865, p. 319; j 
 Quart. Jour. Geol. Soc. Loudon, vol. 21, 1865, p. I 
 482, pi. IB. 
 
 Stylonurus powriei Page, S. scoticus n. s. 
 
 On the discovery of a new genus of > 
 
 Cirripedia in the Weulock limestone, I 
 Dudley. 
 
 In Quart. Jour. Geol. Soc. London, vol. 21, 
 
 1865, p. 486, pi. 14; Geol. Mag., vol. 2, London, 
 
 1865, p. 319. 
 
 Turrilcpas n. g. 
 
VOGDEB.] 
 
 LIST OF AUTHORS. 
 
 75 
 
 Woodward (Henry)— Continued. 
 
 On a new genus of Eurypterida from 
 
 the Lower Ludlow rocks of Leintwar- 
 dine, Shropshire. 
 
 In Quart. Jour. Geol. Soc. London, vol. 21, 
 1865, p. 490, pi. 14. 
 
 Hemiaspis n. g. 
 
 and Salter (J.W.) Chart of the 
 
 genera of fossil Crustacea. See Salter 
 (J. W.) and Woodward (Henry). 
 
 Shield bearing Crustacea, recent 
 
 and fossil. 
 
 In Intellectnral Observer, vol. 8, 1865, p. 321, 
 plate. 
 
 Harpes. 
 
 First report on the structure and 
 
 classification of fossil Crustacea. 
 
 In Kept. 35th Meeting Brit. Assoc. Adv. Sci., 
 
 1865. 
 
 On a new Phyllopodous Crustacean. 
 
 In Kept. 35th Meeting Brit. Assoc. Adv. Sci., 
 
 1865, Trans, of Sec., p. 78. 
 
 Discinocaris n. g., D. browniana Woodward. 
 For description and illustration of Discino- 
 caris, see Quart. Jour. Geol. Soc., vol. 22, 1866. 
 
 On the occurrence of Ceratiocaris in 
 
 the Wenlock limestone of England. 
 
 In Geol. Mag., vol. 3, London, 1866, p. 203, 
 
 pi. 10. 
 
 Note on some fossil Crustacea and a 
 
 Chilognathous Myriapod from the Coal 
 Measures of the west of Scotland. 
 
 In Trans. Geol. Soc. Glasgow, vol. 2, 1866, p. 
 234, pi. 3, wood-cuts. 
 
 On a new genus of Phyllopodous 
 
 Crustacean from the Moffat shales, 
 Dumfriesshire. 
 
 In Quart. Jour. Geol. Soc. London, vol. 22, 
 
 1866, p. 503, pi. 25. 
 
 Discinocaris n. g., L>. browniana , Peltocaris 
 aptychoides. 
 
 See. also, Kept. 35th Meeting Brit. Assoc. 
 Adv. Sci., 1865, Trans, of Sec., p. 78. 
 
 Second report on the structure and 
 
 classification of the fossil Crustacea. 
 
 In Kept. 36th Meeting Brit. Assoc. Adv. Sci., 
 
 1866, p. 71. 
 
 Eurypterida , Xiphosura. 
 
 On some points in the structure of 
 
 the Xiphosura, having reference to their 
 ' relationship with the Eurypteridw. 
 
 In Quart. Jour. Geol. Soc. London, vol. 23, 
 
 1867, p. 28, pis. 1,2. 
 
 Eurypterida: Pterygotus Agas., Slimonia 
 (Page) Woodward, Stylonurus (Page) Wood- 
 ward, Eurypterus De Kay subgenus, Dolichop. 
 terns Hall, Adelopthalmus Jordan, Bunodes 
 Eichw., Arthropleura Jordan, Hemiaspis 
 
 Woodward (Henry)— Continued. 
 
 Wood., Exapinurus Nieszk., Pseudoniscus 
 Nieszk. Xiphosura: Belinurus (Konig) Baily, 
 Prestwichia n. g., Limulus Muller. 
 
 A monograph of the British fossil 
 
 Crustacea of the order Mesostomata. 
 
 In Palaeont. Soc. London, pt. 1, 1866 ; pt. 2, 
 1868; pt.3, 1871; pt. 4, 1872; pt. 5, 1877, 36 pis. 
 
 Pterygotus, Slimonia, Stylonurus, Eurypterus , 
 Hemiaspis, Belinurus , Neolimuhis, Prestwichia, 
 Limulus, Cyclus. 
 
 Third report on the structure and 
 
 classification of the fossil Crustacea. 
 
 In Rept. 37th Meeting Brit. Assoc. Adv. Sci., 
 
 1867, p. 44. _ „ . 
 
 Eurypterus, Pterygotus, Prceatya, Gomocy • 
 
 poda. 
 
 Recent and fossil Crustacea ; being 
 
 a lecture delivered before the Geologi- 
 cal Association, December 12, 1867. 
 
 In Geol. Mag., vol. 5, London, 1868, p. 33; 
 Rept. Geol. Assoc., 1867; notice of lecture. 
 
 On a new Limuloid Crustacean ( Neo - 
 
 limulus falcatus), from the Upper Silu- 
 rian of Lesmahagow, Lanarkshire. 
 
 In Geol. Mag., vol. 5, London, 1868, p. 1, pi. 1. 
 
 On a newly discovered long-eyed 
 
 Calymene from the Wenlock limestone. 
 Dudley. 
 
 In Geol. Mag., vol. 5, London, 1868, p. 489, 
 pi. 21. 
 
 Contributions to British fossil Crus- 
 tacea. 
 
 In Geol. Mag., vol. 5, London, 1868, p. 258; 
 also p. 353, pis. 14, 17. 
 
 Pyrgoma Crustacea, Glyphea , and Pseudogly, 
 phea. 
 
 On some new species of Crustacea 
 
 from the Upper Silurian rocks of Lan- 
 arkshire, etc. ; and further observations 
 on the structure of Pterygotus. 
 
 In Quart. Jour. Geol. Soc. London, vol. 24, 
 1868, p. 289, pis. 9, 10. 
 
 Eurypterus ( Pterygotus ) punctatus Salter, 
 Eurypterus scorpioides n. s., E. obesus n. s. 
 Pterygotus raniceps n. s. 
 
 Fourth report on the structure and 
 
 classification ot the fossil Crustacea. 
 
 In Rept. 38th Meeting Brit. Assoc. Adv. Sci., 
 
 1868, p. 72, pi. 2. 
 
 Neolimulus falcatus sp. et gen. nov., Cyclus 
 radialis Dekon. 
 
 On the occurrence of Stylonurus in 
 
 the “ cornstone ” of Herefordshire. 
 
 In Rept. 39 tb Meeting Brit. Assoc. Adv. Sci., 
 
 1869, Trans, of sec., p. 103. 
 
 | Note on the palpus and other ap- 
 
 pendages of an Asaphus from the Tren- 
 ton limestone in the British Museum. 
 
[bull. 63. 
 
 76 A BIBLIOGRAPHY OP PALEOZOIC CRUSTACEA. 
 
 Woodward (Henry) — Continued. 
 
 In Quart. Jour. Geol. Soc. London, vol. 26, 
 1870, p. 486, wood-cut. 
 
 On the remains of a giant Isopod, 
 
 Prcearcturus gigas, from the Old Red 
 Sandstone of Rowlestone quarry, Here- 
 fordshire. 
 
 In Trans. Woolhope Nat. Field Club, 1870, 
 p. 266, 3 pis. 
 
 On Necrogrammarus salweyi, lower 
 
 Ludlow, Leintwardine. 
 
 In Trans. Woolhope Nat. Field Club, 1870, 
 p. 271. 
 
 On Eurypterus brodiei, from Perton, 
 
 Hereforshire. 
 
 In Trans. Woolhope Field Club, 1870, p. 276, 
 2 pis. 
 
 Notes on fossil Crustacea. 
 
 In Kept. 40th Meeting Brit. Assoc. Adv. Sci., 
 
 1870, Trans, of sec., p. 91. 
 
 Eurypterus , Cemtioca.ru, Cyclus, Dithyro- 
 caris. 
 
 Contributions to British fossil Crus- 
 tacea. 
 
 In Geol. Mag., vol. 7. London, 1870, p. 554, 
 
 pi. 22. 
 
 Cyclus. 
 
 On the structure of Trilobites. 
 
 In Geol. Mag., vol. 8, London, 1871, p. 289, 
 pi. 8. 
 
 Asaphus platycephalus Stokes. 
 
 On some new Phyllopodous Crusta- 
 ceans from the Palaeozoic rocks. 
 
 In Geol. Mag., vol. 8, 1871, p. 104, pi. 3. 
 
 Ceratiocaris, Dithyrocaris. 
 
 Extract published in the Canadian Natural- 
 ist, n. s., vol. 6, 1871, p. 18. 
 
 Fifth report on the structure and 
 
 classification of the fossil Crustacea, 
 etc. 
 
 In Rept. 41st Meeting Brit. Assoc. Adv. Sci., 
 
 1871, p. 53; also, Geol. Mag., vol. 8, London, 
 1871, p. 521. 
 
 On a new species of Eurypterus ( E . 
 
 brodiei) from Perton, near Stoke Edith, 
 Herefordshire. 
 
 In Quart. Jour. Geol. Soc. London, vol. 27, 
 1871, p. 261, figures. 
 
 On a new fossil Crustacean, from the 
 
 Devonian of Canada. 
 
 In Canadian Naturalist, n. s., vol. 6, 1871, 
 
 p. 18. 
 
 Dithyrocaris. 
 
 Note on some British Palaeozoic 
 
 Crustacea belonging to the order Me- 
 sostomata. 
 
 In Geol. Mag., vol. 9, London, 1872, p. 433, 
 
 pi. 10. 
 
 Woodward (Henry) — Continued. 
 
 Hemiaspis , Pseudoniscus , Exapinurus , Buno - 
 des, Bellinurus, Prestwichia. 
 
 Further remarks on the relationship 
 
 of the Xiphosura to the Eurypteridae, 
 and to the Trilobita, etc. 
 
 In Quart. Jour. Geol. Soc. London, vol. 28, 
 1872, p. 46, figures; also, Annals Mag. Nat. 
 Hist. London, 4th series, vol. 9, London, 1872, 
 p. 406. 
 
 Sixth report on the structure and 
 
 classification of the fossil Crustacea, 
 etc. 
 
 In Rept. 42d Meeting Brit. Assoc. Adv. Sci., 
 1872, p. 321; also, Geol. Mag., vol. 9, London, 
 
 1872, p. 563. 
 
 Life forms of the past and present. 
 
 In Popular Sci. Review, vol. 11, London, 
 
 1873, p. 391, pis. 90,91. 
 
 Pterygotus, Slimonia, Stylonurus , Eurypterus, 
 Hemiaspis, Prestwichia, Bellinurus, Neolimu- 
 lus, Dithyrocaris, Trinucleus ornatus, Sao hir . j 
 suta. 
 
 On a new Trilobite from the Cape of 
 
 Good Hope. 
 
 In Quart. Jour. Geol. Soc. London, vol. 29, 
 1873, p. 32, pi. 2. 
 
 Encrinurus crista-galli. 
 
 Seventh report of the committee ap- 
 pointed for the purpose of continuing 
 researches in fossil Crustacea, consisN 
 ing of Prof. P. Martin Duncan, Henry 
 Woodward, and Robert Etheridge. 
 
 In Rept. 43d Meeting Brit. Assoc. Adv. Sci ., 'a 
 1873, p. 304 ; also, Geol. Mag. , vol. 10, London, 
 1873, p. 520. 
 
 Olenus utahensis n. s. 
 
 and Etheridge, jr. (Robert). On 
 
 some specimens of Dithyrocaris , from the 
 Carboniferous limestone series, East ' 
 Kilbride, and the Old Red Sandstone of 
 Lanarkshire. 
 
 In Geol. Mag., vol. 10, London, 1873, p. 482, 
 pi. 16. 
 
 On some specimens of Dithyro- 
 caris, from the Carboniferous limestone j 
 series, East Kilbride, and from the old j 
 red sandstone of Lanarkshire. 
 
 In Rept. Brit. Asso., vol. 43, 1873, Trans, of i 
 sec., p. 92. 
 
 Eighth report on fossil Crustacea. ' 
 
 In Rept. 45th Meeting Brit. Assoc. Adv. Sci., 'J 
 1875 ; also, Geol. Mag., new series, decade 2, vol. j 
 2, 1875, p. 620. 
 
 Two lectures on receut and fossil 
 
 Crustacea delivered at the Royal Insti- 
 tution, on April 29 and May 6, 1876. 
 
 In Proc. Royal Inst. Gr. Brit., 1876; Times, I 
 Morning Post, Illustrated News, 1876. 
 
POGDES.] 
 
 LIST OF AUTHORS, 
 
 77 
 
 Woodward (Henry)— Continued. 
 
 A catalogue of British fossil Crus- 
 tacea, with their synonyms and the 
 range in time of each genus and order. 
 Published by order of the trustees of 
 the British Museum 1877. 
 
 A review of the book was published in the 
 Geol. Mag., decade 2, vol. 4, J877. 
 
 Note on the genus Anthrapalcemon 
 
 ( Pdlceocarabus ) of Salter from the Coal 
 Measures. 
 
 In Geol. Mag., decade 2, vol. 4, 1877, p. 55. 
 
 Article “ Crustacea.” 
 
 In Ency. Britannica, vol. 6, 1877, 86 wood-cuts. 
 
 Asaphus, Trinucleus, Sao, Aridaspis, Para- 
 doxides. 
 
 Discovery of the remains of a fossil 
 
 crab (Decapoda-Br achy ura) in the Coal 
 Measures of the environs of Mons, 
 Belgium. 
 
 In Geol. Mag., decade 2, vol. 5, London, 1878, 
 p. 433, pi. 11. 
 
 Brachypyge carbonis Wood. 
 
 Note on Palaeozoic Crustacea. 
 
 In Geol. Mag., decade 2, vol. 6, 1879, p. 196, 
 
 ! pl-5. 
 
 Eurypterus scouleri. 
 
 \ A new genus of Trilobites Onycopyge 
 
 liver8idgei, from South Wales. 
 
 In Geol. Mag., decade 2, vol. 7, 1880, p. 97, 
 
 figure. 
 
 Note on a new English Homalonotus 
 
 from the Devonian, Torquay, South 
 Devon. 
 
 In GeoLMag., decade'2, vol. 8, London, 1881, 
 p. 489, pi. 13. 
 
 Homalonotus champernownei 
 
 Contributions to the study of fossil 
 
 Crustacea. 
 
 In GeoL Mag., decade 2, vol. 8, London, 1881, 
 p. 529, pi. 14. 
 
 Eryon perroni, Palceocaru burnettii, figure, 
 p. 533, pi. 14, tig. 3. 
 
 Additional note on Homalonotus from 
 
 the Devonian. 
 
 In Geol. Mag., decade 2, vol. 9, London, 1882, 
 
 p. 157, pi. 4. 
 
 Homalonotus goniopygoeus, H. champernow- 
 
 nei. 
 
 I Note on Ellipsocaris deivalquei, a new 
 
 Phyllopod from the Upper Devonian of 
 Belgium. 
 
 In Geol. Mag., decade 2, vol. 9, London, 1882, 
 p. 444, figures. 
 
 On a series of Phyllopod Crustacean 
 
 shields from the Upper Devonian of the 
 
 Woodward (Henry)— Continued. 
 
 Eilel; and on one from the Wenlock 
 shales of Wales. 
 
 In Geol. Mag., new series, decade 2, vol. 9, 
 London, 1882, p. 385, pi. 9. 
 
 Gardiocaris n. g., Pholadocaris n. g., Apty- 
 chopis. 
 
 Synopsis of the genera and species 
 
 of Carboniferous limestone Trilobites. 
 
 In Geol. Mag. . new series, decade 2, vol. 10, 
 London, 1883, pp. 445, 481, 534, pis. 11-13. 
 
 Phillip8ia, Griffithides, Brachymetopus. 
 
 Edition by author 3 pis. and 26 pp. 
 
 Synonyms of Phillipsia gemmulifera. 
 
 In Geol. Mag., decade 3, vol. 1, London, 1884 
 
 p. 22. 
 
 Monograph of the British Carbonif- 
 erous Trilobites. 
 
 In Palaeont. Soc. London, pt. 1, 1883, pp. 1-38, 
 pis. 1-6. Phillipsia , Griffithides. Pt. 2 (conclu- 
 sion), 1884, pp. 39-83, pis. 7-10. 
 
 Proetus, Phillipsia , Brachymetopus , Griffi- 
 thides, Dalmanites? . 
 
 On the structure of Trilobites. 
 
 In Geol. Mag., decade 3, vol. 1, London, 1884, 
 p. 78. 
 
 Asaphus. 
 
 Appendages of Trilobites. 
 
 In Geol. Mag., decade 3, vol. 1, London, 1884, 
 
 p. 162. 
 
 Asaphus megistos , 2 figs. ; Oalymene. 
 
 Note on the remains of Trilobites 
 
 from South Australia. 
 
 In Geol. Mag., decade 3, vol. 1, London, 1884, 
 p. 342. 
 
 Conocephalites , Dolichometopus . 
 
 Synopsis of the genera and species 
 
 of Carboniferous limestone Trilobites. 
 
 In Geol. Mag., decade 3, vol. 1, London, 1884, 
 p. 484, pi. 16. 
 
 Phillipsia laticaudata, P. scabra, P. carinata , 
 Griffithides brevispinus, G. glaber, G. ? carring- 
 tonensis. 
 
 On the discovery of Trilobites in the 
 
 Culm shales of southeast Devonshire. 
 
 In Geol. Mag., decade 3, vol. 1, 1884, p. 534. 
 
 Phillipsia lei, P. minor, P. cliffordi, P. articu- 
 losa. 
 
 and Jones (T. Rupert). Notes on 
 
 the phyllodiform Crustacea, referable 
 to the genus Edinocaris, from the Pa- 
 laeozoic rocks. 
 
 In Geol. Mag., decade 3, vol. 1, London, 1884, 
 p. 393, pi. 13. 
 
 Ceratiocari8. 
 
 On some Palaeozoic Phyllopod shields 
 
 and on Nebalia and its allies. 
 
 In Geol. Mag., decade 3, vol. 2, London, 1885, 
 p. 345, pi. 9. 
 
78 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Woodward (Henry) — Continued. 
 
 Notice of a new limuloid Crustacean 
 
 from the Devonian, by H. S. Williams. 
 
 In Geol. Mag., decade 3, vol. 2, London, 1886, 
 p. 427. 
 
 On the discovery of Trilobites in the 
 
 Upper Green (Cambrian) slates of the 
 Penrhyn quarries, Bethesda, near Ban- 
 gor, North Wales. 
 
 In Quart. Jour. Geol. Soc. London, vol. 44, 
 1888, p. 74, pi. 6. 
 
 Oonocoryphe viola Wood. 
 
 On the discovery of Trilobites in the 
 
 Upper Green (Cambrian) slates, etc., 
 North Wales. 
 
 In Rept. 57 tli Meeting Brit. Assoc. Adv. Sci., 
 1887, p. 696. 
 
 Conocoryphe viola. 
 
 On a new species of Eurypterus from 
 
 the Lower Carboniferous shale, Esk- 
 dale, Scotland. 
 
 In Rept. 57th Meeting Brit. Assoc. Adv. Sci., 
 1887, p. 696. 
 
 See Jones (T. Rupert) and Wood- 
 ward (H$nry). 
 
 See Etheridge (Robert) and Wood- 
 ward (Henry). 
 
 Worthen (A. H.) Description of two 
 new species of Crustacea, fifty-one spe- 
 cies of mollusca, and three species of 
 Crinoids from the Carboniferous forma- 
 tion of Illinois and adjacent States. 
 
 In Bull. No. 2 State Mus. Nat. Hist. Hlinois, 
 1884. 
 
 Colpocaris Chester ensis, Solenocaris St.Ludo- 
 vici. 
 
 See also Meek (F. B.) and Worthen (A. H.) 
 
 Young (J.) Descriptive notes of several 
 new and rare forms of Entomostraca. 
 
 In Trans. Geol. Soc. Glasgow, vol. 5, pt. 2, 
 1877. 
 
 On the Silurian strata of Pen- 
 
 whapple Glen, near Girvan. 
 
 In Proc. Nat. Hist. Soc. Glasgow, vol. 1, pt. 2, 
 1868, p. 171; also in Proc. Royal Phys. Soc. Edin- 
 burgh, vol. 4, 1878. 
 
 Solenocaris n. g. (not Solenocaris Meek.). 
 
 Zenker (J. C.) Beitrage zur Naturge- 
 schichte der Urwelt. Organische Reste 
 
 Zenker (J. C.) — Continued. 
 
 (Petrefacten) rus der Altenburger 
 Braunkohlen-Formation, dem Blanken- 
 burger Quadersandstein, jenaischen 
 bunten Sandstein und bohmischen 
 Uebergangsgebirge, mit 6 illuminirten 
 Kupfertafeln. Jena, 1833. 
 
 Olenus longicaudatus, O. pyramidalis, O. 
 latus, Otarion n. g., O. diffractum, O. ? squar- 
 rosum, Oonocephalus n. g., C. costatus, Ellipso- 
 cephalus n. g., E. ambiguus. 
 
 The genus Otarion was made up from the 
 head of Oyphaspis burmeisteri Barr., connected 
 with the pygidium of Gromits beamonti Barr. 
 The second species, described as Otarion f 
 squarrosum , is referred by Joachim Barrande 
 to Cheirurus quenstadi. 
 
 J. C. Zenker uses two generic names for his 
 new genus Oonocephalus, the first on p. 48 in 
 describing the genus and the second in his de- 
 scription of plate 5, where he calls it Trigono- 
 cephalus. 
 
 Both these generic terms had been used in 
 natural history for other genera, the first by 
 Thurnburg in 1812 for a genus of the Orthop- 
 tera, and the second by Oppel in 1811 for the 
 Reptiles. 
 
 The typical species described as Oonocephalus 
 costatus on p. 49, and also in the explanation of 
 pi. 5, figs. G-K, p. 51, and as Trigonocephalus 
 costatus in the description of pi. 5, given on p. 
 51, has been referred by Joachim Barrande to 
 an amended genus, Conocephalites (Zenker) 
 Barr., and the species to the older name of 
 sulzeri. The other new genus, Ellipsocephalus, 
 has been used by all subsequent authors. 
 
 Zeno (Franz). Yon Seeversteinerungen 
 und Fossilien, welche bei Prag zu finden 
 Sind. 
 
 In Nene phys. Belustigungen, etc., vol. 1, 
 1770, p. 65. Continued same vol., p. 362, pi. 1, 
 fig. 1. 
 
 Under the names of Cacada or K'dfermuschcl 
 Franz Zeno describes the pygidium of Dal- 
 manites hausmanni and the head of Phacops 
 latifrons. 
 
 Zittel (Karl A.) Handbuch der Palseon- 
 tologie. Vol. 2. Miinchen und Leip- 
 zig, 1881-’85, p. 525. 
 
 ! Zippe (F. X.) See Sternberg (Kasper 
 | Graf yon). 
 
PART II. 
 
 CATALOGUE OF TRILOB1TES, 
 
PART II 
 
 A SYSTEMATIC CATALOGUE OF AMERICAN PALEOZOIC CRUSTACEA, 
 
 TRILOBITA. 
 
 First series , with grooved pleurae. 
 
 Family. 
 
 Genera. 
 
 Reference. 
 
 Harpedidm 
 
 Harpes Goldfuss, 1839 
 
 Nova Acta Physico-Med., vol. 19, p. 358. Type, 
 Harpes macroceplialus Gold., Harpes ungula 
 Sternb. Barrande, Syst. Sil. Boheme, vol. 1; p. 
 347, pis. 3-9. 
 
 Remopleuridfe . 
 
 Remopleurides Portlock, 1843 
 
 Geol. Rept. Londonderry, etc., p.254. Type, Be- 
 mopleurides colbii Portlock. 
 
 Paradoxidae 
 
 Paradoxides Brongniart, 1822 
 
 Hist. Crust. Foss., p. 30. Type, Paradoxides tes- 
 sini Brong. 
 
 
 Anopolenus Salter, 1864 
 
 Geol. Soc. London Jour., vol. 20, p. 236. Type, 
 
 
 
 Anopolenus henrici Salter. 
 
 
 Bathynotus Hall, 1860 
 
 Thirteenth Rept. New York 'State Cab. Nat. 
 Hist., p. 117. Type, Bathynotus holopyga Hall. 
 
 
 Dicellocephalus Owen, 1852 
 
 Rept. Geol. Survey Wisconsin, Iowa, and Minne- 
 sota, p. 573. Type, Dikelocephalus minnesotensis 
 
 Owen. 
 
 
 Mesonacis Walcott, 1884 
 
 Am. Jour. Sci., 3d series, vol. 29, p. 329. Type, Ole- 
 nus vermontana Hall. 
 
 
 Dolichometopus Angelin, 1854 
 
 Palseont. Scand., p. 72. Type, Dolichometopu 
 svecicus ; Ang. Palseont. Scand., p. 73, pi. 37, 
 
 fig. 9. 
 
 
 Hydrocephalus Barrande, 1846 
 
 Notice Pr61im. Syst. Sil. Bohfime, p. 18. Type, 
 Hydrocephalus carens Barr. Notice Pr61im. 
 Syst. Sil. Boheme, p. 19. 
 
 
 Olenellns Hall, 1861 
 
 Fifteenth Rept. New York State Cab. Nat. Hist., 
 p. 114. Type, Olenellus thompsoni Hall. Twelfth 
 Rept. Now York State Cab. Nat. Hist., p. 59, 
 figure. 
 
 
 Olenus Dalman, 1826 
 
 Palaead., p. 56. Type, Olenus gibbosus Wahlen- 
 bnrg. 
 
 
 Zacanthoides Walcott, 1887 
 
 Am. Jour. Sci., 3d scries, vol. 36, p. 165. Typo, 
 Olenoides spinosus Walcott. 
 
 
 Parabolina Salter, 1849 
 
 Mem. Geol. Survey United Kingdom, decade 2. 
 Type, Olenus spimdosa Wahl. 
 
 
 I’eltura Milno-Edwards, 1840 
 
 Hist. Nat. Crust., vol. 3, p. 344. Typo, Olemcs 
 
 
 
 scarabcenides Wahl. 
 
 
 Cyclognathus Linnarsson, 1875 . . . 
 
 Geol. Foreuingens Stockholm Forhandl., vol. 2, 
 No. 12, p. 500. Type, Cyclognathus mioropygus 
 Linnarsson. 
 
 81 
 
 Bull. 63 6 
 
82 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 First series, grooved pleurae— Continued. 
 
 Family. 
 
 Genera. 
 
 Reference. 
 
 Paradoxides . . - 
 
 Triarthrus Green, 1832 
 
 Mon. Trilobites North America, p. 87. Type, 
 Triarthrus beckii Green. 
 
 
 Leptoplastus Angelin, 1854 
 
 Subgenera: 
 
 Pakeont. Scand., p. 46. Type, Leptoplastus steno- 
 tus Angelin. 
 
 
 1. Sphserophtkalmus Angelin, 
 
 Palaeont. Scand., p. 49. Type, Sphcerophthalmus 
 
 
 1854. 
 
 flagellifer Aug. 
 
 
 2. Ctenopyge Linnarsson, 1880. 
 
 Geol. Fdreningens Stockholm Forhandl., vol. 5, p. 
 145. Type, Olenus ( Sphcerophthalmus ) pecten 
 
 
 . 
 
 Salter. 
 
 
 Bceckia Brogger, 1882 
 
 Die silurischeD Etagen 2 und 3, p. 122. Type, 
 
 
 
 Bceckia hirsuta Brogger. 
 
 
 Ceratopyge Corda, 1847 
 
 Prodr., p. 161. Type, Olenus for ficular Sara. 
 
 Bohemillidas . . . 
 
 Bohemilla Barrande, 1872 
 
 Svst. Sil. Bolifime, vol. 1, Snppl., p. 137. Type, 
 
 
 
 Bohemilla stujrenda Barr. 
 
 Conocoryphidte 
 
 Atops Emmons, 1844 
 
 Taconic System, p. 20. Type, Atops trilineatus 
 Emmons. 
 
 
 Conocorvphe Corda, 1847 
 
 Prodr., p. 23. Type, Trilobite sulzeri Schlutt. 
 
 
 Ptychoparia Corda, 1847 
 
 Prodr., p. 26. Type, Conocephalus striatus. 
 
 
 Ctenocephalus Corda, 1847 
 
 Prodr., p. 26. Type, Ctenocephalus barrandi 
 Corda. 
 
 
 Solenopleura Angelin, 1854 
 
 Paheont. Scand., p. 26. Type, Solenopleura holo- 
 metopa Ang. 
 
 
 Liostracus Angelin, 1854 
 
 Palaeont. Scand., p. 27. Type, Liostracus aculea- 
 tus Angelin. 
 
 
 Aneuacanthus Angelin, 1854 
 
 Palteont. Scand., p. 5. Type, Aneuacanthus acu- 
 tangulus A ng. 
 
 
 Anomocare Angelin, 1854 
 
 Palaeont. Scand., p. 24. Type, Anomocare aculea- 
 tus Angelin. 
 
 
 Angelina Salter, 1847 
 
 Mem. Geol. Survey United Kingdom, decade xi. 
 Type Angelina sedgwicki Salter. 
 
 
 Agraulos Corda, 1847 
 
 Prodr., p. 26. Agraulus certicephalus Bair. 
 
 
 Dorypyge Dames, 1884 
 
 China (Richthofen), vol. 4, p. 23. 
 
 
 Bathyurus Billings, 1859 
 
 Canadian Naturalist, vol. 4. p. 364. Type, Asaphus 
 extans Hall. 
 
 
 Bathyurella Billings, 1865 
 
 Pal. Foss., vol. 1, p. 262. B. marginatus, B. niti 
 dus, B. expansus Billings. 
 
 
 Chariocephalus Hall, 1863 
 
 Sixteenth Rept. New York State Cab. Nat. Hist., 
 p. 175. Type, Chariocephalus whitfieldi Hall. 
 
 
 Corynexochus Angelin, 1854 
 
 Paheont. Scand., p. 59. Type, Corynexochus spinu- 
 
 
 Ellipsocepbalus Zenker, 1833 
 
 losa Ang. 
 
 
 Beitrage Nat. Urwelt, p. 31. Type, Ellipsoce- 
 
 
 
 phalus ambiguus Zonker^Ellipsocephahis hoffi 
 Schlott. 
 
 
 Ptycbaspis Hall, 1863 
 
 Sixteenth Rept. New York State Cab. Nat. Hist., 
 p. 170. Type, Bikelocephalus minisccensis Qwen. 
 
 
 Sao Barrande, 1846 
 
 Notice Prdlim. Syst. Sil. Bohdmo, p. 13. Type. 
 Sao hirsuta Barr. 
 
 
 
 
 
 
VODGES.] 
 
 CATALOGUE OF TRILOBITES. 
 
 83 
 
 First series, with grooved pleurae — Continued. 
 
 Family. 
 
 Genera. 
 
 Reference. 
 
 
 
 Mem. Soc. Geol. France, vol. 1, p. 355. Type, 
 Proetus cuvieri Steininger. 
 
 
 
 
 Declienella Kayser, 1880 
 
 Zeitschr. Deutscli. geol. Gesell., Berlin, vol. 32, p. 
 703. Type, Dechenella verneuili Barr. 
 
 
 Prionopeltis Corda, 1847 ( Phceton 
 
 Prodr., p. 121. Type, Prionopeltes polydorus 
 
 
 Barr., Phcet7wnid.es Angelin), 
 
 Corda. 
 
 
 Bracliymetopus McCoy, 1847 
 
 Annals Mag. Nat. Hist., 1st series, London, vol. 
 20, p. 229. Type, Phillipsia maccoyi Portlock. 
 
 
 Cyphaspis Burmeister, 1843 
 
 Org. Trilobiten (Bay Soc. Ed., p. 98). Pliacops 
 certophthalma Gold. 
 
 
 Aretliusina Barrande, 1852 
 
 Syst. Sil. Boheme, vol. 1, p. 494. Arethusina ko- 
 nincki Barr. 
 
 
 Harpides Beyrich, 1846 
 
 TJntersuch. Trilobiten, p. 34. Type, Harpides 
 hospes Beyrich. 
 
 
 Cannon Barrande, 1872 
 
 Syst. Sil. Boheme, vol. 1, suppl., p. 19. Type, Gar- 
 mon multilus Barr. 
 
 
 Cyplioniscus Salter, 1852 
 
 Kept. 22d Meeting Brit. Assoc. Adv. Sci., Trans. 
 Sec., p. 95. Type, Cyphoniscus socialis Salter. 
 
 Phillipsidae .... 
 
 Pliillipsinella Novak, 1885 
 
 Sitzungshe. rbokm. Gesell. Wiss., 1885. Author’s 
 edition, p. 4. Type, Phillipsinella parabola 
 Barr. 
 
 
 Phillipsia Portlock, 1843 
 
 Geol. Kept. Londonderry, etc., p. 305. Type, 
 Phillipsia kelli Portlock =Asaphus gemmulifera 
 Phillips. 
 
 
 Griffithides Portlock, 1843 
 
 Geol. Kept. Londonderry, etc., p. 310. Type, 
 Griffithides longiceps Portlock. 
 
 Dalmanitidas .. 
 
 Pliacops Emmrich, 1839 
 
 De Trilob., etc., p. 18. Type, Phacops latifions 
 Bronn. 
 
 
 Dalmanites Emmrich, 1844 
 
 Zur Nat. Trilobiten, etc., p. 15. Barrande’s Syst. 
 Sil. BohSme, vol. suppl., p. 27. Type, Dalmani- 
 tes caudata Briinnich. 
 
 
 Coronnra Hall & Clarke, 1888 
 
 Pal. New York, vol. 7, p. xxxii. Type, Coronnra 
 aspectens Conrad. 
 
 
 Cryph®us Green, 1837 
 
 Am. Jour. Sci., 1st series, vol. 32, p. 343. Type, 
 Cryphoeus boothi Green. 
 
 
 Chasmops McCoy, 1849 
 
 Annals Nat. Hist., 2d series, vol. 4 ; also Contrib. 
 to Pal®ont., p. 143. Type, Calymene odini 
 Eichwald. 
 
 Calymenid® . . . 
 
 Calymeno Brongniart, 1822 
 
 Crust. Foss., p. 11. Type, Calymene tuberculata 
 Briinnich. 
 
 
 Homalonotus Koenig, 1825 
 
 leones Foss. Sectilos, p. 7. Typo, Homalonotus 
 
 
 
 knighli Koenig. 
 
 
 Bavarilla Barrande, 1868 
 
 Fauue Sil. des environs de Hof on Bavidre, p. 75. 
 Typo, Bavarilla ho/ensis Barr. 
 
 Licliasid® 
 
 Lichas Dalman, 1826 
 
 Palaiad., p. 53. Type, Lichas laciniatus WaJjl. 
 
84 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 First series , with grooved pleurae — Continued. 
 
 Family. 
 
 Genera. 
 
 Reference. 
 
 Trinucleid® . . . 
 
 Trinucleus Lhlwyd, 1698 (Crypto- 
 lithus Green, 1832). 
 
 Ampyx Dalman, 1826. 
 
 Murchison’s Silurian Syst., 1839, p. 659. Type, 
 Trinucleus fimbriatus. 
 
 Pal* ad., p. 53. Type, Ampyx nasuta Dalman. 
 Neues Jahrb. fur Mineral., 1847, pt. 4, p. 391 ; Syst. 
 Sil. Boheme, vol. 1, p. 540. Type, Dionidce for- 
 mosa Barr. 
 
 Mem. Geol. Survey United Kingdom, decade xi, 
 pi. 7, p. 1. Type, Salteria primceva Thomson. 
 
 ! Pal. Foss., vol. 1, p. 93. Type, Endyminia meeki 
 1 Billings. 
 
 
 Subgenera : 
 
 1. Saltcria Thomson, 1864 
 
 2. Endymima Billings, 1862... 
 
 
 
 Syst. Sil. BohOme, vol. 1, p. 663. Typo, AEglina 
 rediviva Barr. 
 
 
 
 IllaBnurid* — 
 
 
 Sixteenth Kept. New York State Cab. Nat. Hist., 
 p. 176. Type, lllcenurus quxdratus Hall. , 
 
 
 Asaphid® 
 
 Asaphus Brongniart, 1822 
 
 Crust. Foss., p. 17. Type, Asaphus expansus 
 Wahl. 
 
 Palseont. Scand., p. 51. Type, Ptychopyge appa- 
 nata Ang. 
 
 Mon. Brit. Trilobites, p. 167. Type, Asaphus recti- 
 frons Portlock and Asaphus Icevigatus Angelin. 
 
 Palaeont. Scand. , p. 15. Type, Megalaspis gigas 
 Angelin. 
 
 Crust. Foss., p. 26. Type, Asaphus buehi Brong. 
 
 Annals Nat. Hist., 2d series, vol. 4, p. 409. Type, 
 Barrandia cordai McCoy. 
 
 Palaeont. Scand., p. 13. Type, Asaphus frontalis 
 Dalman. 
 
 Quart. Jour. Geol. Soc. London, vol. 33, p. 663. 
 Type, Asaphellus homfrayi Salter. 
 
 Palsead., p. 49. Type, Xileus armadillo Dalman. 
 
 
 Brachyaspis Salter, 1866 
 
 
 Megalaspis Angelin, 1852 
 
 
 Ogygia Brongniart, 1822 
 
 
 Barrandia McCoy, 1849 
 
 
 Niobe Angelin, 1852 
 
 
 Asaphellus Callaway, 1877 
 
 
 Nilens "Dalman, 1826 
 
 
 
 Second series, with plane pleurae. 
 
 Stvginidse 
 
 St, yginia Salter 1853 
 
 Kept. 22d Meeting Brit. Assoc. Adv. Sci., p. 59. 
 Type, Styginia latifrons Portlock. 
 
 
 
 Illsenidse 
 
 Illaenus Dalman, 1826 
 
 Palsead., p. 51. Type, Illcenus crassicauda Wahl. ; 
 Nova Acta Reg. Soc. Sci. Upsal., vol. 8, p. 27, pi. 
 2^ figs. 3, 5,6. (Not. pi. 7, figs. 5, 6 = Illcenus 
 esmarki.) 
 
 Organization Trilobites, p. 105 (Ray Soc. Ed. 
 
 1846). Type, Dysplanus centrotus Dalm. 
 
 Sil. Syst , p. 656. Type, Bumastus barriensis 
 Murch. 
 
 M6m. Acad. Sci. Sr.-Petersbourg, 7th series, vol. 6, 
 No. 2, p. 31. Type, Panderia triquetra Volb. 
 
 
 Dysplanus Burmeister, 1843 
 
 
 Bumastus Murchison, 1839 
 
 
 Panderia Yolborth, 1863 
 
V0GDE6. ] 
 
 CATALOGUE OF TRILOBITES. 
 
 85 
 
 Third series, with ridged pleurae ( pleure a bourrelet, Barrande). 
 
 Family. 
 
 Genera. 
 
 Reference. 
 
 Acidaspidae — 
 
 Acidaspis Muichison, 1839 ( Odon - 
 topleura Emmrich, 1839). 
 
 Silurian System, p. 558. Type, Acidaspis brightii 
 Murch. 
 
 Ceraurid® 
 
 Ceraurus Green, 1832 ( Oheirurus 
 Beyrich, 1845). 
 
 Spk^rexochus Beyrich, 1845 
 
 Mon. Trilobites N. A., p. 83. Type, Ceraurus 
 pleurexanthemus Green. 
 
 TTeber einige bohm. Trilobiten, p. 19. Type, Sphee- 
 rexochus mirus Beyrich. 
 
 Syst. Sil. BohOrne, vol. 1, suppl., p. 96. Type, Areia 
 bohemica Barr. 
 
 Syst. Sil. Boheme, vol. 1, p. 814. Type, Deiphon 
 forbesi Barr. 
 
 Prodr., p. 128. Type, Placoparia zippi Boeck. 
 
 Syst. Sil. Boheme, vol. 1, p. 810. Type, Stauro- 
 cephalus murchisoni Barr. 
 
 Geol. Mag., decade 2, vol. 7, p. 97. Type, Onyco- 
 pyge liver sidgei Woodward. 
 
 
 
 
 
 
 Staurocephalus Barrande, 1852 
 
 Ony copy ge Woodward, 1880 
 
 Amphionid®. . 
 
 Amphion Pander, 1850 
 
 Beitrage Geog. Russischen Reiches, p. 439. Type, 
 Amphion fischeri Eichwald. 
 
 Syst. Sil. Boheme, vol. 1, p. 821. Type, Cromus in- 
 tercostatus Barr. 
 
 Cronins Barrande, 1852 
 
 
 
 Encrinurid®... 
 
 Encrinurus Emmrich, 1844 (Cryp- 
 tonymus Eichwald). 
 
 Cybele Eoven, 1845 
 
 Zur Nat. Trilobiten, p. 16. Type, Trilobus punc- 
 tatus Briinnich. 
 
 Sven ska Akad. Fbrhandl., 1845, p. 110. Type, 
 Calymene bellatula Dalman. 
 
 Prodr., p. 119. Type, Dindymene frederico-au- 
 gusti Corda. 
 
 
 Dindymene Corda, 1847 
 
 
 
 Brontid® 
 
 BronteuS Goldfuss, 1843 
 
 Beitrage Petrefact., Nova Acta Physico-Med., 
 vol. 19, p. 360. Type, Brontes flabellifer Gold. 
 
 Fourth series. 
 
 Agnostid® 
 
 Agnostus Brongniart, 1822 
 
 Hist. Crust. Foss., p. 38. Type, Agnostus pisi - 
 
 formis. 
 
 Shumardia Billing3, 1862 Pal. Foss., vol. 1, p. 92. Type, Shumardia granu- 
 
 losa Billings. 
 
 Microdiscus Emmons, 1856 Am. Geology, vol. 1, pt. 2, p. 116. As defined by 
 
 . Chas. D. Walcott, 1886. Type, M. punctatus 
 
 and M. speciosus. 
 
A CATALOGUE OF NORTH AMERICAN SPECIES OF TRILOBITES, 
 
 {Current names are printed in bold face type; synonyms in Italic .] 
 
 Acantlioloma Conrad, 1840; 3d Annual Rept. Pal. Dept. New York Geol. Survey, 
 p. 205. (See Acidaspis.) 
 
 spinosa Conrad. (See Acidaspis tuberculatus.) 
 
 Acidaspis Murchison, Silurian System, 1839, p. 658. 
 
 Type, Acidaspis brightii Murch., Sil. Syst., p. 658, pi. 14, figs. 10, 15. 
 
 Syn., Cer atocephala Warder, 1838; Am. Jour. Sci., 1st series, vol. 34, p. 377. 
 Odontopleura Emmrich, 1839; De Tril., p. 53. 
 
 Arges Goldfuss (iu part), Neues Jahrbuch fur Miueral., 1843, pp. 544,556. 
 Polyeris Rouault, 1846; Bull. Soc. G6ol. France, vol. 4, p. 320. 
 
 Selenopeltis Corda, 1847 ; Prodr., p. 34. 
 
 Trapelocera Corda, 1847 ; Prodr., p. 158. 
 
 Discranurus Conrad, 1841 ; 5tli Ann. Rept. Pal. Dept. New York Geol. 
 Survey, p. 48. 
 
 anchoralis Miller, 1875; Cincinnati Quart. Jour. Sci., vol. 2, p. 349, figs. 2-4. 
 
 Hudson. 
 
 armatn8. (See Acidaspis eriops.) 
 
 callicera Hall, 1888 ; Pal. New York, vol. 7, pp. 69, 224, pi. 16 b, figs. 1-3. 
 
 Upper Heidelberg. 
 
 [ Ceratocephala ] ceralepta Anthony, 1838; Am. Jour. Sci., 1st series, vol. 34, p. 
 
 379, figs. 1, 2 Hudson. 
 
 ceralepta Meek, 1873; Pal. Ohio, vol. 1, p. 169, pi. 14, figs. 8-9. 
 
 ceralepta Miller, 1874; Cincinnati Quart. Jour. Sci., vol. 1, p. 130. 
 
 cincinnatiensis Meek, 1873 ; Pal. Ohio, vol. 1, p. 167, pi. 14, fig. 3. Hudson. 
 
 cincinnatiensis Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 130. 
 
 [ Ceraurus] crosotus Locke, 1842; Am. Jour. Sci., 1st series, vol. 44, p. 347, fig. 
 
 Hudson. 
 
 crosotus James, 1871 ; Catalogue Fossils Cincinnati Group, p. 14. 
 
 crosotus Meek, 1873; Pal. Ohio, vol. 1, p. 165, pi. 14, figs. 10 a, b. 
 
 crosotus Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 129. 
 
 danai Hall, 1862; Geol. Wisconsin, vol. 1, p. 432. Niagara. 
 
 Syn., Acidaspis ula (Wincliell and Marcy) Hall, 20tli Rept. New York State Cab. 
 Nat. Hist.,p. 389. 
 
 danai Hall, 1867; 20tli Rept. New York State Cab. Nat. Hist., p. 333, pi. 21, 
 
 figs. 8, 9. 
 
 danai Hall, 1870 ; 20th Rept. New York State Cab. Nat. Hist., p. 423, pi. 21, figs. 
 
 8, 9 (rev. ed.). 
 
 [ Terataspis ] eriops Hall, 1876; Illus. Devonian Foss. Crust., pi. 19, figs. 4-7,10, 
 
 11, 12. (See Lichas ( Conolichas ) eriops Hall.) 
 
 fimbriata Hall, 1879; Description of New Species from the Niagara Group, p. 
 
 20. Niagara. 
 
 fimbriata Hall, 1882; Trans. Albuny Inst., vol. 10, p. 76. 
 
 . 87 
 
88 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63. 
 
 Acidaspis flxnbriata Hall, 1883; lltli Rept. Geol. Nat. Hist. Indiana, p. 334, pL 33, 
 fig. 11. 
 
 [ Terataspis ] grandis Hall, 1870; Ulus. Devonian Foss. Crust., pi. 17, figs. 1-8; 
 
 pi. 18, figs. 1-4. (See Licha.s ( Terataspis ) grandis Hall.) 
 
 lialli Shumard, 1855 ; 1st and 2d Rept. Geol. Survey Missouri, pt. 2, p. 200, pi. B, 
 
 figs. 7 a. lb, c. Trenton. 
 
 [ Discranurus ] harnata Conrad, 1841; 5th Ann. Rept. Pal. Dept. New York Geol. 
 
 Survey, p. 48, pi. 1, fig. 1. Lower Helderberg. 
 
 [ Discranurus ] hamata Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., 
 
 pi. 2, fig. 1. Republicatiou of pi. 2, 5th Ann. Rept. Pal. Dept. New York Geol. 
 Survey. 
 
 hamafa Hall, 1859; Pal. New York, vol. 3, p. 371, pi. 79, figs. 15-19. 
 
 hamata Meek and Worthen, 1868; Geol. Survey Illinois, vol. 3, p. 390, pi. 7, fig. 17. 
 
 horani Billings, 1857; Geol. Survey Canada, p. 341. Trenton. 
 
 horani Billings, 1863; Geol. Survey Canada, p. 190, fig. 190. 
 
 ida Winchell and Marcy, 1865; Mem. Boston Soc. Nat. Hist., vol. 1, p. 106, pi. 3, 
 
 fig. 13. 
 
 o’nealli Miller, 1875; Cincinnati Quart. Jour., vol. 2, p. 86, fig. 9. Hudson. 
 
 ortoni Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 90, pi. 8, fig. 1. 
 
 parvula Walcott, 1877 ; Advanced sheets 31st Rept. New York State Mus., p. 16. 
 
 Trenton. 
 
 parvula Walcott, 1879 ; 31st Rept. New York State Mus., p. 69. 
 
 romingeri Hall, 1888; Pal. New York, vol. 7, pp. 71,224, pi. 16 b, figs. 15-18. 
 
 Hamilton. 
 
 spiniger. .,(Seo Bathyurus spiniger.) 
 
 trentonensis Hall, 1847 ; Pal. New York, vol. 1, p. 240, pi. 64, figs. 4 af. 
 
 Trenton. 
 
 trentonensis Emmons, 1855 ; American Geology, vol. 1, pt. 2, p. 216, fig. 73. 
 
 tuberculatus Conrad, 1840; 3d Ann. Rept. Pal. Dept. New York Geol. Survey, 
 
 p. 205. # Lower Helderberg. 
 
 Syn., Acantholoma Conrad, 1840; 3d Ann. Rept. Pal. Dept. New York Geol. Sur- 
 vey, p. 205, fig. 3. 
 
 Acantholoma spinosa Conrad, 4th Ann. Kept. Pal. Dept. New York Geol. 
 Survey, p. 39, pi. 1, fig 3. 
 
 tuberculatus Hall, 1859; Pal. New York, vol. 3, p. 368, pi. 79, figs. 1-14. 
 
 tuberculatus Hall, 1861 ; 15th Rept. New York State Cab. Nat. Hist., pi. 2, fig. 3. 
 
 Actinurus De Castelnau, 1843; Sil. Syst. de PAm6r., p. 21. (See Lichas boltoni.) 
 Aglaspis Hall, 1862 ; Canadian Naturalist, vol. 7, p. 445, figure. Hall, 1863 ; 16th 
 Rept. New York State Cab. Nat. Hist., p. 181. 
 
 Type, Aglaspis harrandi Hall. 
 
 barrandi Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 181, pi. 11, 
 
 figs. 7-16. Potsdam. 
 
 eatoni Whitfield, 1880; Ann. Rept. Geol. Survey Wisconsin, p. 52. Potsdam. 
 
 eatoni Whitfield, 1882 ; Geol. Wisconsin, vol. 4, p. 192, pi. 10, fig. 11. 
 
 Agnostus Brongniart, 1822; Hist. Nat. Crust. Foss., p. 38. 
 
 Type, Agnostus pisiformis, idem., p. 38, pi. 4, figs. 4 a, 4 b. 
 
 Syn., Battus Dalman, 1826; Palsead., p. 33. 
 
 Trinodus McCoy, 1846 ; Sil. Foss. Ireland, p. 56. 
 
 Phalacroma Corda (in part), 1847 ; Prodr., p. 158. 
 
 Mcsosphcniscus Corda, 1847 ; Prodr., p. 46 ( Agnostus integer ). 
 
 Diplorrhina Corda, 1847 ; Prodr., p. 46. 
 
 Condglopgge Corda, 1847 ; Prodr., p. 50 (Agnostus rex). 
 
 Lejopyge Corda, 1847 ; Prodr., p. 51 (Agnostus Icevigatus). 
 
 Arlhrorhachis Corda, 1847 ; Prodr., p. 114 (Agnostus tardus ). 
 
 Pcronopsis Corda, 1847; Prodr., p. 115 (Agnostus interger). 
 
 . Pleuroctenium Corda, 1847; Prodr., p. lift (Agnostus grannlatus). 
 
V0GDE8.] 
 
 CATALOGUE OF TRILOBITES. 
 
 89 
 
 Agnostus acadicus Hartt, 1868 ; Acadian Geology, p. 655, fig. 229 (3d ed.). St. John. 
 Syn., Similis Hartt, 1868; Acadian Geology, p. 656 (3d ed.). 
 
 Similis Hartt (Walcott), 1884 ; Bull. U. S. Geol. Survey, No. 10, p. 22. 
 
 acadicus Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 22, pi. 2, figs. 2, 2 
 
 a, c. 
 
 americauus Billiugs, 1860 ; Canadian Naturalist, vol. 5, p. 302, fig. 1. Quebec. 
 
 americanus Billings, 1865 ; Pal. Foss., vol. 1, p. 395, fig. 372. 
 
 bidens Meek, 1873 ; 6th Ann. Rept. U. S. Geol. Survey Territories, p. 463. 
 
 Potsdam. 
 
 bidens Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 26, 
 
 pi. 9, figs. 13, 13 a. 
 
 canadensis Billings, 1860 ; Canadian Naturalist, vol. 5, p. 304, fig. 3. Quebec. 
 
 canadensis Billings, 1865 ; Pal. Foss., vol. 1, p. 397, fig. 374. 
 
 coloradoensis Shumard, 1861 ; Am. Jour. Sci., 2d series, vol. 32, p. 218. 
 
 Potsdam. 
 
 communis Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par., vol. 4, p. 228, 
 
 pi. 1, figs. 28, 29. Potsdam. 
 
 communis Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 27. 
 
 disparlis Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 179, pi. 10, 
 
 figs. 25-27. Potsdam. 
 
 fabius Billings, 1865; Pal. Foss., vol. 1, p. 298, fig. 289. Quebec. 
 
 glabba Billings, 1865 ; Pal. Foss., vol. 1, p. 297, fig. 288. Quebec. 
 
 interstrictus White, 1874; Prelim. Rept. Invert. Foss., p. 7. Potsdam. 
 
 interstrictus White, 1877 ; U. S. Geog. and Geol- Survey W. 100th Meridian, p. 
 
 38, pi. 2, figs. 5 a, 5 b. 
 
 interstrictus Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 149, pi. 16, 
 
 figs. 6, 6 a. 
 
 interstrictus Walcott, 1888 ; Am. Jour. Sci., 3d series, vol. 36, p. 166. 
 
 sp.? Rominger, 1887; Proc. Acad. Nat. Sci. Phila., p. 18. 
 
 josepha Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 178, pi. 6, 
 
 figs. 54, 55. Potsdam. 
 
 lobatus Hall. (See Microdiscus lobatus.) 
 
 maladensis Meek, 1873 ; 6th Annual Rept. U. S. Geol. Survey Territories, p. 464. 
 
 Calciferous. 
 
 neon Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par., vol. 4, p. 229, pi. 1, 
 
 figs. 26,27. Potsdam. 
 
 neon Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 27. 
 
 nobilis Ford, 1872 ; Am. Jour. Sci., 3d series, vol. 3, p. 421, figs. 1,2. Postdam. 
 
 nobilis Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 150, pi. 16, fig. 7. 
 
 orion Billings, 1860; Canadian Naturalist, vol. 5, p. 304, fig. 2. Quebec. 
 
 orion Billings, 1865; Pal. Foss., vol. 1, p. 397, fig. 393 
 
 orion Shnrnard, 1863; Trans. Acad. Sci. St. Louis, vol. 2, p. 105. 
 
 parilis Hall, 1863 ; 16th Rept. New York State Cab. Nat. Hist., p. 179, pi. 11, figs. 
 
 23, 24. Potsdam. 
 
 prolongus Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par., vol. 4, p. 230, 
 
 pi. 1, figs. 30, 31. Potsdam. 
 
 prolongus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S Geol. Survey, vol. 8, p. 28. 
 
 richmondensis Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 
 
 8, p. 24, pi. 9, fig. 10. Cambrian. 
 
 seclurus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 25, 
 
 pi. 9, fig. 14. Cambrian. 
 
 similis Hartt. (See Agnostus acadicus.) 
 
 tumidosus Hall and Whitfield, 1877; U. S. Geol. Expl. 40th Par., vol. 4, p. 231, 
 
 pi. 1, fig. 32. Potsdam. 
 
90 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 I BULL. 63. 
 
 Agraulos Corda, 1847; Prodr., p. 23. 
 
 Typo, Arionellus certicephalus Barrande. 
 
 Syn., Avion Barrande, 1846; Notice Prdlim., p. 13. 
 
 Ellipsocephalus Barrande, 1846; Notice Prdlim., p. 12 (not Ellipsocephalus 
 Zenker) or ( Elliptocephalus Emmons). 
 
 Arionellus Barrande, 1852; Syst. Sci. Boheme, p. 404. 
 
 affinis Billings, 1874; Pal. Foss., vol. 2, p. 72. Potsdam. 
 
 affinis Matthew, 1886; Traus. Royal Soc. Canada, vol. 2, p. 153, figs, 2, 2 a, b. 
 
 [ Arionellus ] bipunctatus Shumard, 1863; Trans. Acad. Sci. St. Louis, vol. 2, p. 
 
 101. Potsdam. 
 
 [ Arionellus ] bipunctatus Hall, 1863 ; 16tk Kept. New York State Cab. Nat. 
 
 Hist., p. 169, pi. 7, figs. 50-57. 
 
 [ Arionellus ( Agraulos )] convexus Whitfield, 1878; Ann. Rept. Geol. Survey 
 
 Wisconsin, 1877, p. 57. Potsdam. 
 
 [ Arionellus'] convexus Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 190, pi. 1, 
 
 fig. 17. 
 
 [ Arionellus ] cylindricus Billings, 1860; Canadian Naturalist, vol. 5, p. 314, fig. 
 
 14. Quebec. 
 
 [ Arionellus'] cylindricus Billings, 1865; Pal. Foss., vol. 1, p. 406, fig. 385. (See 
 
 Ptychaspis cylindricus.) 
 
 ? globosus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 61, pi. 9, fig. 23. Cambrian. 
 
 oweni Meek and Hayden, 1861; Proc. Acad. Nat. Sci. Phila., 1861, p. 436. 
 
 Potsdam. 
 
 The s*pecies was also referred to the genera Arionellus and Crepicephalus. 
 
 [Arionellus ] oweni Meek and Hayden, 1862; Atn. Jour. Sci., 2d series, vol. 33, 
 
 p. 74. 
 
 [ Arionellus ] oweni Meek and Hayden ; Pal. Upper Missouri, p. 9, figs, a, b, c, 
 
 pi. 1, fig. 4. 
 
 Referred by Walcott, 1884, Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 
 8, p. 55, pi. 10, to Ptychoparia oweni. 
 
 [Arionellus ( Bathyurus )] planus Shumard, 1861; Am. Jour. Sci., 2d series, vol. 
 
 32, p. 219. Potsdam. 
 
 [ Arionellus ] pustulatus Walcott, 1877 ; Advanced sheets 31st Rept. New York 
 
 State Mus. Nat. Hist., p. 15. Chazy. 
 
 [Arionellus'] pustulatus Walcott, 1877; 31st Rept. New York State Mus. Nat. 
 
 Hist., p. 68. 
 
 [ Arionellus ] quadrangularis Whitfield, 1884; Bull. Mus. Nat. Hist. New York, 
 
 vol. 1, p. 147, pi. 14, fig. 8. Potsdam. 
 
 quadrangularis Walcott, 1884 ; Bull. U. S. Geol. Survey, No. 10, p. 48, pi. 7, fig. 1. 
 
 socialis Billings, 1874; Pal. Foss., vol. 2, p. 71, fig. 40. Potsdam. 
 
 socialis Matthew, 1886; Trans. Royal Soc. Canada, vol. 2, p. 151, fig. 1, 1 a, b. 
 
 strenuus Billings, 1874; Pal. Foss., vol. 2, p. 71, fig. 41. Potsdam. 
 
 strenuus Matthew, 1886 ; Trans. Royal Soc. Canada, vol. 2, p. 153, figs. 3, 3 a, b. 
 
 subclavatus Billings. (See Ptychaspis subclavatus.) 
 
 [ Arionellus ( Bathyurus )] texanus Shumard, 1861 ; Am. Jour. Sci., 2d series, vol. 
 
 32, p. 218. Potsdam. 
 
 [ Arionellus] tripunctatus Whitfield, 1876; Rept. Recon. Upper Missouri, p. 141, 
 
 pi. 1, figs. 3-5. Potsdam. 
 
 [Bathyurus?] woosteri Whitfield, 1878; Ann. Rept. Geol. Survey Wisconsin, 
 
 1877, p. 56. Potsdam. 
 
 [Bathyurus?] woosteri Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 189, pi. 1, 
 
 figs. 19-21. 
 
 Amphion Pander, 1830 ; Beitriige zur Geol. russischen Reiches, p. 139. 
 
 Type, Amphion fisclieri Eichwald. 
 
VOODES.j 
 
 CATALOGUE OF TRlLOBITES 
 
 91 
 
 Quebec. 
 
 Chazy. 
 
 Quebec. 
 
 Quebec. 
 
 Quebec. 
 
 Quebec. 
 
 166 , 
 Trenton. 
 Cbazy. 
 
 Quebec. 
 
 Quebec. 
 
 Quebec. 
 
 Quebec. 
 
 Amphion barrandi Billings, 1865; Pal. Foss., vol. l,p. 288, fig. 277. 
 
 — - canadensis Billings, 1859; Can. Nat., vol. 4, p. 381, fig. 12, a, b. 
 
 canadensis Billings, 1863 ; Gcol. Survey Canada, p. 133, fig. 69. 
 
 canadensis Billings, 1865; Pal. Foss., vol. 1, p. 288, fig. 278. 
 
 convexus Billings, 1865 ; Pal. Foss., vol. 1, p. 322. 
 
 insularis Billings, 1865; Pal. Foss., vol. 1, p. 290. 
 
 julius Billings, 1865; Pal. Foss., vol. 1, p. 290, fig. 279. 
 
 matutina Hall, 1863; 16th Kept. New York State Cab. Nat. Hist., p. 222, pi. 5 a, 
 
 fig. 6. Potsdam. 
 
 multisegment atus. (See Encrinurus multisegmentatus.) 
 
 nevadensis Walcott, 1884; Pal. Eureka Dist. Mon. U. S. Geol. Survey, vol. 8, p. 
 
 94, pi. 12 ; fig. 13. Pogonip. 
 
 salteri Billings, 1861 ; Canadian Naturalist, vol. 6, p. 322, fig. 6. Calciferous. 
 
 salteri Billings, 1865 ; Pal. Foss., vol. 1, p. 352, fig. 399. 
 
 westoni Billings, 1865 ; Pal. Foss., vol. 1, p. 321, fig. 307. 
 
 Ampyx Dalman, 1826; Palaead., p. 53 (German edition). 
 
 Type, Ampyx nasuta Dalman. 
 
 americanus Safford and Yodges, 1889; Proc. Phila. Acad. Nat. Sci., p 
 
 figure. 
 
 halli Billings, 1861 ; Pal. Foss., vol. 1, p. 24, figs. 25, a, b, c. 
 
 halli Billings, 1862; Geol. Survey Vermont, vol. 2, p. 959, fig. 365. 
 
 laeviusculus Billings, 1865; Pal. Foss., vol. 1, p. 295, fig. 285. 
 
 tiormalis Billings, 1865; Pal. Foss., vol. 1, p. 295, fig. 286. 
 
 rustilius Billings, 1865 ; Pal. Foss., vol. 1, p. 296. 
 
 semicostatus Billings, 1865; Pal. Foss., vol. 1, p. 297, fig. 287. 
 
 Angelina Salter, 1864 ; Mem. Geol. Survey United Kingdom, decade xi, pi. 7. 
 
 Type, Angelina sedgwicki Salter. 
 
 hitchcocki Whitfield, 1884; Bull. Am. Mus. Nat. Hist., New York, vol. 1, p. 
 
 148, pi. 14, fig. 13. (See Frotypus hitchcocki.) Potsdam. 
 
 Anomocare Angelin, 1852 ; Palseont. Scand., p. 24. 
 
 Type, Anomocare aculeatus Ang., pi. 18, fig. 6. 
 
 [? Conoceph.] depressus Shumard, 1861; Am. Jour. Sci., 2d series, vol. 32, p. 
 
 219. Potsdam. 
 
 [ Lonchocephus] hamulus Owen, 1852; Geol. Survey Wisconsin, Iowa, and Min- 
 nesota, p. 576, pi. 1 a, figs. 8-12. Potsdam. 
 
 undet. Trilobite, Owen, 1848 ; Geol. Reconnoissance Chippewa Land Dist., p. 
 
 15, pi. 7, fig. 5. 
 
 [ Conocephalites] hamulus Shumard, 1863; Acad. Sci. St. Louis, vol. 2, p. 104. 
 
 [ Conoceplmlites] hamulus Hall, 1863; 16th Kept. New York State Cab. Nat. 
 
 Hist., p. 166, pi. 7, figs. 43,44; pi. 8, figs. 25,26. 
 
 hamulus Dames, 1884 ; China (Richthofen), vol. 4, p. 24. 
 
 [Conocephalites] patersoni Hall, 1863; Rept. New York State Cab. Nat. Hist., p. 
 
 159, pi. 7, figs. 45, 46. Potsdam. 
 
 patersoni Dames, 1884 ; China (Richthofen), vol. 4, p. 24. 
 
 ? parvum Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 59, pi. 9, fig. 17. * Cambrian. 
 
 ? parvum Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 209, pi. 25, 
 
 fig. 1. 
 
 [Crcpicephalus ?] wisconsensis Owen, 1852; Rept. Geol. Survey Wisconsin, 
 
 Iowa, and Minnesota, pi. 1, fig. 13. (The upper figure only ; the other figured 
 specimen belongs to Dikelocephalus granulosus.) 
 
 [Crepicephalu8] wisconsensis Shumard, 1863; Trans. Acad. Sci. St. Louis, vol. 
 
 2, p. 103. 
 
92 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63 . 
 
 Anomocare [ Crepicephalus} wisconsensis Hall, 1863; 16tli Rept. New York State 
 Cab. Nat. Hist., p. 164, pi. 7, figs. 39-41 ; pi. 8, tigs. 22, 23, 24, 27, 28. 
 
 Syn., Dikelocephalus latifrons (Shumard) Hall, 1863; 16tli Rept. New York State 
 Cab. Nat. Hist., p. 165, pi. 7, fig. 40. 
 
 wisconsensis Dames, 1884; China (Richthofen), vol. 4, p. 24. Potsdam. 
 
 Anopolenus Salter, 1864; Geol. Mag., vol. 1, jj. 236. 
 
 Type, Anopolenus henrici Salter ; Quar. Jour. Geol. Soc. London, vol. 20, p. 236, pi. 
 13, figs. 4, 5. (See, also, Anopolenus salteri Hicks ; same journal, vol. 
 21, p. 478, pi. , fig. 1. 
 
 venustus Billings, 1874 ; Pal. Foss., vol. 2, p. 73, fig. 42. Potsdam. 
 
 Arethusina Barrande, 1852 ; Syst. Sii. Boheme, vol. 1, p. 493. 
 
 Type, Arethusina konincki Barrande. 
 
 americana Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 62, pi. 9, fig. 27. Cambrian. 
 
 Arges. (See Lichas.) 
 
 Arges, subgenus Lichas, Hall and Clarke, 1888 ; Pal. New York, vol. 7, p. lx. 
 
 phlyctanodes Green. (See Lichas phlyctanodes. ) 
 
 arionellus. (See Agraulos.) 
 
 Asaphiscus Meek, 1873 ; 6th Ann. Rept. U. S. Geol. Survey Territories, p. 485 (foot- 
 note). 
 
 \_Bathyurellus ( Asaphiscus )] bradleyi Meek, 1873; 6th Ann. Rept. U. S. Geol. 
 
 Survey Territories, p. 484. Cambrian. 
 
 bradleyi Meek, 1873; 6th Ann. Rept. U. S. Geol. Survey Territories, p. 485. 
 
 wkeeleri Meek ; 1873; 6th Rept. U. S. Geol. Survey Territories, p. 485 (foot- 
 note). • Cambrian. 
 
 wheeleri White, 1875; Geog. and Geol. Survey West 100th Meridian, vol. 4, p. 43, 
 
 pi. 2, figs. 1 a-f. 
 
 wheeleri Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 220, pi. 31, figs. 3,3 a.* 
 
 Asaphus Brongniart, 1822; Hist. Nat. Crust. Foss., p. 18, pi. 2, fig. 1 a, b. 
 
 Type, Asaphus expansus Linn6. 
 
 Syn., Cryptonymus, Eichwald, 1825; (in part) not Cryptonymus Eichwald, 1840. 
 Isotelus De Kay, 1822; Annals Lyceum Nat. Hist. New York, vol. 1, p. 174. 
 Hemicrupturus Green, 1832; Mon. Tril. North America, p. 20. 
 
 acantholeurus. (See Dalmanites acantholeurus.) 
 
 alacer Billings, 1866; Catalogue Sil. Foss. Anticosti, p. 26, fig. 9. 
 
 aspectans. (See Dalmanites aspectans.) 
 
 astragalotes Green, 1834; Am. Jour. Sci., 1st series, vol. 25, p. 335. 
 
 astragalotes Green, 1835; Suppl. Mon. Tril. N. A., p. 11, cast 37. 
 
 Probably Phacops rana Green. 
 
 barrandi. (See Ogygia barrandi.) 
 
 canadensis Chapman, 1856; Canadian Jour., vol. 1, p. 482. Utica Slate. 
 
 canadensis Chapman, 1858; Canadian Jour., vol. 2, p. 47. 
 
 canadensis Chapman, 1858; Canadian Jour., vol. 3, p. 230, figure. 
 
 canadensis Chapman, 1859; Canadian Jour., vol. 4, p. 1, figure. 
 
 canadensis Chapman, 1859; Annals Nat. Hist., 3d series, vol. 2, p. 9, fig. 1. 
 
 canadensis Billings, 1863 ; Geol. Survey Canada, p. 204, fig. 201. 
 
 From a personal study of the species collected on the Georgian Bay, Canada, " 
 I am inclined to refer Asaphus halli and A. hincksii to Asaphus canadensis 
 Chapman. 
 
 [ Isotelus ] canalis Conrad MSS. Chazy. } 
 
 [ Isotelus *] canalis Hall, 1847; Pal. New York, vol. 1, p. 25, pi. 4 bis, figs. 17-19. 
 
 canalis Billings, 1865; Pal. Foss., vol. 1, p. 255; also p. 352, fig. 340 (not Con- 
 rad sp.). 
 
 canalis Billings, 1862; Geol. Vermont, vol. 1, p. 299, pi. 12, fig. 5. 
 
 This species is probably Asaphus platycephalus. 
 
CATALOGUE OF TRJLOBITES. 
 
 vogdes. | 
 
 93 
 
 Asaphus canalis Whitfield, 1886; Bull. Am. Mus. Nat. Hist., New York, vol. 1, p. 
 336, pi. 34, figs. 1-8. 
 
 canalis Whitfield, 1889 ; Bull. Am. Mus. Nat. Hist., New York, vol. 2, p. 64, 
 
 pis. 11, 12. 
 
 caribouensis Walcott, 1884; Pal. Eureka Dist.,Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 98, pi. 12, figs. 7-7 a, b. Pogonip. 
 
 caudaius. (See Dalmanites limulurus.) 
 
 cordieri. (See Dalmanites limulurus.) 
 
 corycoeus. (See Proetus corycceus.) 
 
 crypturus. (See Homalonotus crypturus.) 
 
 curiosus Billings, 1865; Pal. Foss., vol. 1, p. 318, fig. 305. Quebec. 
 
 ? curiosus Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 98, pi. 12, fig. 15. 
 
 denticulatus. (See Dalmanites denticulatus. ) 
 
 ditmarsice Houeyman, 1879 ; Proc. Nova Scotia Inst. Nat. Sci., vol. 5, p. 18. 
 
 (See Homalonotus crypturus Green.) Clinton? 
 
 duirus Green, 1839; Am. Jour. Sci., 1st series, vol. 37, p. 40. Hudson. 
 
 edicardi. (See Dalmanites limulurus.) 
 
 emoryi Hall, 1857 ; Rept. U. S. Mexican Boundary Survey, vol. 1, pi. 20, fig. 5. 
 
 Not defined. 
 
 sxtans. (See Bathyurus extans.) 
 
 gigas. (See Asaphus platycephalus.) 
 
 [Megalaspis? ] goniocercus Meek, 1873 ; 6th Ann. Rept. U. S. Geol. Survey Ter- 
 ritories, p. 480. Quebec. 
 
 goniurus Billings, 1860; Canadian Naturalist, vol. 5, p. 324. Quebec. 
 
 goniurus Billings, 1865; Pal. Foss., vol. l,p. 415. 
 
 halli. (See Cryphaeus boothi.) 
 
 halli Chapman, 1858; Annals Nat. Hist., 3d series, vol. 2, p. 14, fig. 2. 
 
 Trenton and Utica. 
 
 halli Chapman, 1858; Canadian Jour., 2d series, vol. 3, p. 236, figure. 
 
 This species is the same as Asaphus canadensis Chapman. 
 
 hincksii Chapman, 1859 ; Canadian Jour. Industry, Sci. and Arts, vol. 4, p. 2, 
 
 figure. (See Asaphus canadensis Chapman.) Utica. 
 
 homalononotoides Walcott, 1877 ; Advanced sheets 31st Rept. New York State 
 
 Mus. Nat. Hist., p. 20. Trenton. 
 
 homalononotoides Walcott, 1879 ; 31st Rept. New York State Mus. Nat. Hist., 
 
 p. 71. 
 
 homalononotoides Whitfield (not Walcott), 1882; Geol. Wisconsin, vol. 4, p. 237. 
 
 (See Asaphus triangulatus.) 
 
 huttoni Billings, 1865; Pal. Foss., vol. 1, p. 271, fig. 256. Quebec. 
 
 illsenoides Billings, 1860 ; Canadian Naturalist, vol. 5, p. 323. 
 
 illeenoides Billings, 1865 ; Pal. Foss., vol. 1, p. 414. 
 
 [Isotelus] iowensis Owen, 1852; Rept. Geol. Survey Wisconsin, Iowa, and Min- 
 nesota, p. 577, pi. 2 a, figs. 1-7. Trenton. 
 
 laticostatus. (See Dalmanites anchiops.) 
 
 ? latimarginata Hall, 1847 ; Pal. New York, vol. 1, p. 253, pi. 66, figs. 4 a, b. 
 
 Utica. 
 
 limulurus. (See Dalmanites limulurus.) 
 
 marginalis Hall, 1847 ; Pal. New York, vol. 1, p. 24, pi. 4 his, fig. 15. Chazy. 
 
 marginalis Emmons, 1855; Am. Geology, vol. 1, pt. 2, p. 235, pi. 3, fig. 16. 
 
 - — llsotelns ] maximus Locke, 1838; 2d Ann. Rept. Geol. Survey Ohio, p. 246, figs. 
 
 Trenton and Hudson. 
 
 Syn., Isotelus megistos Locke, 1841; Trans. Am. Assoc. Geol. Nat., p. 221, pi. 6. 
 Isoteius megistos Locke, 1842; Am. Jour. Sci., 1st series, vol. 42, p. 366, pi. 3. 
 
94 
 
 A BIBLIOGRAPHY OP PALEOZOIC CRUSTACEA. 
 
 [hull. 03 . 
 
 Syn., Isotelus megistos Meek, 1873; Pal. Ohio, vol,l, p. 157, pi. 14, fig. 13. 
 
 Isotelus megistos Miller, 1874, Cincinnati Quart. Jour. Sci., vol. 1, p. 137. 
 Asaphus megistos Walcott, 1884; Science, Marcli 7, fig. 1, vol. 3, p. 200. 
 Asaphus megalopthalmus Troost, 1840; 5tli Geol. Rept. Tennessee, p. 57. 
 
 Trenton ? 
 
 micropleurus Green, 1835; Suppl. Mon. Tril. North America, p. 21, cast No. 41. 
 
 micrurus. (See Dalmanites micrurus.) 
 
 morrisi Billings, 1865; Pal. Foss., vol. 1, p. 272, fig. 257, Syn. to Asaphus huttoni 
 
 Billings. 
 
 murchisoni Castelnau, Syn. to Asaphus platycephalus Stokes. 
 
 myrmecophorus. (See Dalmanites myrmecophorus. ) 
 
 nasutus. (See Dalmanites nasutus.) 
 
 ? nodostriatus Hall, 1847; Pal. New York, vol. 1, p. 248, pi. Cl, figs. 1 a, b. (See 
 
 Bathyurus extans Hall.) 
 
 notans Billings, 1866 ; Catalogue Silurian Foss. Anticosti, p. 25, fig. 8. 
 
 Compare Asaphus maximus Locke. 
 
 ? obtusus Hall, 1847 ; Pal. New York, vol. 1, p. 24, pi. 4 bis, fig. 14. Chazy. 
 
 obtusus Emmons, 1855 ; American Geology, vol. 2, pt. 2, p. 236, pi. 3, fig. 14. 
 
 pelops Billings, 1865 ; Pal. Foss., vol. 1, p. 317, fig. 304. Quebec 
 
 platycephalus Stokes, 1823 ; Trans. Geol. Soc. London, 2d series, vol. 1, p. 208, 
 
 pi. 27. Trenton. 
 
 Syn., Isotelus gigas De Kay, 1824; Annals Lyceum Nat. Hist. New York, vol. 1, p. 
 176, pi. 12, fig. 1. 
 
 Is ot el us planus De Kay, 1824; Annals Lyceum Nat. Hist. New York, vol. 1, 
 p. 1^8, pi. 13, fig. 7. 
 
 Asaphus gigas Dalman, 1826; Palsead.,p. 70. 
 
 Asaphus gigas and planus Dalman, 1826 ; Palsead., p. 70. 
 
 Isotelus gigas Green, 1832 ; Monthly Am. Jour. Geol., p. 560. 
 
 Isotelus gigas Green, 1832 ; Mon. Tril. N. A., p. 71, cast 21, 22. 
 
 Isotelus planus Green, 1832; Monthly Am Jour. Geol., p. 560; Mon. Tril. N. 
 A., p. 68, cast 23. 
 
 Isotelus stegops Green, 1832; Mon. Tril. N. A., p. 71; cast 26, 27. 
 
 Brongniartia isotelea Eaton, 1832; Geological Text Book, p. 33, pi. 2, fig. 22. 
 
 platycephalus Broun, 1835; Lethaea Geogn., vol. 1, p. 115, pi. 9, fig. 8. 
 
 Syn., Isotelus gigas Milne-Edwards, 1840 ; Crust., vol. 3, p. 298. 
 
 platycephalus Buckland, 1840 ; Bridgw. Treatise, vol. 2, p. 76, pi. 63, fig. 12. 
 
 platycephalus Burmeister, 1843; Org. Trilobites, p. 110, pi. 2, fig. 12 (Ray Soc. 
 
 ed., 1846). 
 
 Syn., Isotelus gigas Portlock, 1843; Geol. Rept. Londonderry, p. 295, pi. 7, fig. 1; 
 pi. 8, fig. 1. 
 
 Isotelus planus Portlock, 1843 ; Geol. Rept. Londonderry, p. 295, pi. 7, figs. 
 2, 3. 
 
 Isotelus gigas Hall, 1847 ; Pal. New York, vol. 1, p. 231, pis. 60-63. 
 
 Isotelus gigas Emmons, 1855; Am. Geology, vol. 1, pt. 2, p. 215, pi. 16, fig. 12. 
 
 [ Isotelus ] platycephalus Broun and Roemer, 1851-56; Lethma Geogn., vol. 1, 
 
 p. 632, pi. 9, fig. 8 ; pi. 9 1 , fig. 5. 
 
 platycephalus Nieszkowski, 1857; Mon. Sil. Ostseeprovinz, Tril., p. 37. 
 
 Syn., Isotelus gigas Rogers, 1858 ; Geol. Survey Pennsylvania, vol. 2, p. 819, fig. 610. 
 
 platycephalus Billings, 1863 ; Geol. Survey Canada, p. 184, fig. 183. 
 
 Syn., Asaphus ( Isotelus ) gigas Salter, 1864 ; Mou. Brit. Tril., p. 161, pi. 24, figs.. 1-5; 
 pi. 25, fig. 1 (var.). 
 
 Asaphus ( Isotelus ) gigas Salter, 1864; Mem. Geol. Survey United Kingdom, 
 decade xi, pi. 3. 
 
VOGDES.] 
 
 CATALOGUE OF TKILOBITES. 
 
 95 
 
 Asaphus platycephalus Billings, 1870 ; Quart. Jour. Geol. Soc. London, vol. 26, p. 
 486, pis. 31, 32. 
 
 Syn., Isotelu3 gigas Miller, 1874; Cincinnati Quart. Jour. Sci., vol. l,p. 138. 
 
 platyleurus Green, 1837; Am. Jour. Sci., 1st series, vol. 32, p. 169. (SeeDal- 
 
 manitis platyleurus. ) 
 
 polypleurus Green, 1838; Am. Jour. Sci., 1st series, vol. 34, p. 380. 
 
 quadraticaudatus Billings, 1865; Pal. Foss., vol. 1, p. 273, fig. 258. Quebec. 
 
 rcemingeri Walcott, 1876; 28th Kept. New York State Mus. Nat. Hist., p. 96. 
 
 Trenton. 
 
 selenurus. (See Dalmanites selenurus.) 
 
 stokesi. (See Froetus stokesi.) 
 
 susae Calvin ; MSS. 
 
 susae Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 236, pi. 5, fig. 3 ; pi. 10, fig. 8. 
 
 Trenton. 
 
 tetragonocephalus Green, 1834 ; Am. Jour. Sci., 1st series, vol. 25, p. 135. 
 
 tetragonocephalus Green, 1835; Suppl. Mon. Tril. N. A., p. 12, cast 38. 
 
 [ Paradoxides ] tetragonocephalus Emmrich, 1839; De Tril., etc., p. 34. 
 
 The cast issued with Dr. Green’s monograph as No. 38 may be the same 
 species which Dr. Emmons afterwards described as Atops trilineatus. It .has 
 about sixteen segments in the thorax, also obscure nodes along the axis. The 
 head shows the occular ridges of a Ptyclwparia, whereas the segments are those 
 characterise of the Oleni. It is too imperfect for generic classification. 
 
 trentonensis. (See Lidias trentonensis.) 
 
 triangulatus Whitfield, 1880 ; Ann. Rept. Geol. Survey Wisconsin, 1879, p.59. 
 
 Trenton. 
 
 This species is the Asaphus homalonotoides of the Final Report, vol. 4, p. 237, 
 
 pi. 5, fig. 4. 
 
 ? trimblii Green, 1837 ; Acad. Nat. Sci. Phila., Jour., vol. 7. Niagara. 
 
 trimblii Green, 1837 ; Am. Jour. Sci., 1st series, vol. 32, p. 348. 
 
 LOgygia ?] vetustus Hall, 1847 ; Pal. N. Y., vol. 1, p. 227, pi. 60, fig. 1. 
 
 Trenton and Hudson. 
 
 ? lOgygia ] vetustus Emmons, 1855; Am. Geology, vol. 1, pt. 2, p. 216, fig. 72. 
 
 [ Isotelus] vigilans Meek and Worthen, 1870 ; Proc. Acad. Nat. Sci. Phila., p. 53. 
 
 Hudson. 
 
 llsotelus] vigilans Meek and Worthen, 1875; Geol. Illinois, vol. 6, p. 491, pi. 23, 
 
 fig. 6. 
 
 wisconsensis Walcott, 1876; 28th Rept. N. Y. State Mus. Nat. Hist., p. 97. 
 
 Trenton. 
 
 Aspidolites Conrad, 1841 ; 4th Ann. Rept. Pal. Dept. New York Geol. Survey, p. 48. 
 Atops Emmons, 1844 ; Taconic System, p. 20. 
 
 Type, Atops trilineatus Emmons. 
 
 trilineatus Emmons 1844 ; Taconic System, p. 20, fig. 1, pi. 2, fig. 3. Taconic. 
 
 trilineatus Emmons, 1847; Nat. Hist. New York, Agriculture, vol. 1, p. 64, fig. 8, 
 
 pi. 14, fig. 3. 
 
 Syn., Cahjniene beckii Hall, 1847 ; Pal. New York, vol. 1, p. 252, pi. 67, figs. 4 a-4 e 
 (not Cahjniene beckii Green, or Atops trilineatus Emmons). 
 
 trilineatus Haldeman, 1848; Am. Jour. Sci., 2d series, vol. 5, p. 107. 
 
 trilineatus Emmons, 1849; Proc. Am. Assoc. Adv. Sci., 1st Meeting, Phila., 1848, 
 
 pp. 16, 17. 
 
 Syn., Calymenc beckii Fitch, 1849; Trans. Agric. Soc. New York, vol. 9, p. 865 
 (not Calymene beckii Green). 
 
 trilineatus Emmons, 1855 ; Am. Geology, vol. 1, pt. 2, p. 115, pi. 1, fig. 16. 
 
 Syn., Atops punctatus Emmons, 1860; Manual Geology, p. 88, fig. 71; aiso p. 
 
 280. 
 
96 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63 . 
 
 Atops trilineatus Barrande, 1861 ; Ball. Soc. G6ol. France, 2d series, vol. 18, p. 269, 
 pi. 5, fig. 1. 
 
 trilineatus Barrande, 1861 ; Bull. Soc. G6ol. France, 2d series, vol. 18, p. 271, pi. 
 
 5, fig. 3. 
 
 [ Conocephalites ( Atops )] trilineatus Ford, 1871; Am. Jour. Sci., 3d series, vol. 
 
 2, p. 33. 
 
 [Conocephalites] trilineatus Ford, 1873 ; Am. Jour. Sci., 3d series, vol. 6, p. 135. 
 
 [ Conocephalites (Atops)] trilineatus Ford, 1879; Am. Jour. Sci., 3d series, vol. 9, 
 
 p. 205. 
 
 [ Triarthrus ] trilineatus Miller, 1877 ; Catalogue Am. Pal. Foss., p. 223. 
 
 [Conocoryphe] trilineatus Ford, 1880; Am. Jour. Sci., 3d series, vol. 19, p. 152. 
 
 Syn., Triarthrus beclci Walcott, 1879; Trans. Albany Inst., vol. 10, p. 23. 
 
 [ Ptycoparia ] trilineatus Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 203, 
 
 pi. 27, fig. 1 a-c. 
 
 I Conocoryphe'] trilineatus Walcott, 1887 ; Am. Jour. Sci., 3d series, vol. 34, p. 
 
 197, pi. 1, fig. 7 a, b. 
 
 Bailiella Matthew, 1884; Trans. Royal Soc. Canada, vol. 1, p. 124 (used as a subgenus 
 to Conocoryphe ( Bailiella ) Baileyi). 
 
 Barrandia Hall, 1860; 13th Rept. New York State Cab. Nat. Hist., p. 115 (not Bar- 
 randia McCoy). (See Olenellus.) 
 
 thompsoni. (See Olenellus thompsoni.) 
 
 v ennontana. (See Olenellus vermontana and Mesonasis vermontana.) 
 
 Barrandia McCoy, 1849; Annals Nat. Hist., 2d series, vol. 4, p. 409. 
 
 Type, Barrandia cordai McCoy. 
 
 ? mccoyi Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 96, 
 
 pi. 12, fig. 5. Pogonip. 
 
 Bathynotus Hall, 1860; 13th Rept. New York State Cab. Nat. Hist., p. 117. 
 
 Type, Bathynotus holopyga Hall. 
 
 \_Peltura ( Olenus )] holopyga Hall, 1859; 12th Rept. New York State Cab. Nat. 
 
 Hist., p. 61, figure. 
 
 [Peltura ( Olenus )] holopyga Hall, 1859 ; Pal. New York, vol. 3, p. 528, figure. 
 
 Syn., Paradoxides? quadrispinosus Emmons, 1860; Manual Geology, p. 80, fig. 57. 
 Paradoxides ( Pagura ) quadrispinosus Emmons, 1860; Manual Geology, p. 
 280, fig. 57. 
 
 holopyga Hall, 1860; 13th Rept. New York State Cab. Nat. Hist., p. 118, figure. 
 
 holopyga Hall, 1861 ; Geol. Vermont, vol. 1, p. 371, pi. 13, fig. 3. 
 
 [Peltura (Olenus)] holopyga Barrande, 1861 ; Bull. Soc. G6ol. France, 2d series, 
 
 vol. 18, p. 278, pi. 5, figs. 9, 10. 
 
 holopyga Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 191, pi. 31, figs. 
 
 1-1 a. Middle Cambrian. 
 
 Bathyurellus Billings, 1865; Pal. Foss., vol. 1, p. 262. 
 
 abruptus Billings, 1865 ; Pal. Foss., vol. 1, p. 263, fig. 247. Quebec. 
 
 [ Asaphiscus] hradleyi Meek. (See Asaphiscus bradleyi.) 
 
 expansus Billings, 1865 ; Pal. Foss., vol. 1, p. 318, figs. 306 a, b. Quebec. 
 
 Compare B. nitidus and B. marginatus Billings. 
 
 formosus Billings, 1865; Pal. Foss., vol. 1, p.265, fig. 250. Quebec. 
 
 fraternus Billings, 1865; Pal. Foss., vol. 1, p. 267, fig. 251. Quebec. 
 
 The head of this species may belong to Salter’s genus Siygina. 
 
 litoreus Billings, 1865; Pal. Foss., vol. 1, p. 320. Quebec. 
 
 marginatus Billings, 1865; Pal. Foss., vol. 1, p. 263, fig. 248. Quebec. 
 
 Compare B. nitidus and B. expansus Billings. 
 
 nitidus Billings, 1865; Pal. Foss., vol. 1, p. 265, fig. 249. Quebec. 
 
 On page 320 Mr. Billings says that it may be found necessary to unite B. 
 nitidus, B. marginatus, and B. expansus into one polymorphic species. 
 
VOGDES 1 
 
 CATALOGUE OF TRILOBITES. 
 
 97 
 
 Bathyurellus rarus Billings, 1865; Pal. Foss., 'vol. 1, p. 320, no lignre. Quebec. 
 — — [ Dikelocephalus ] truncatus Meek, 1873; 6tli Ann. Rept. Geol. Survey Terri- 
 tories, p. 465 (no description given). 
 
 validus Billings, 1865 ; Pal. Foss., vol. 1, p. 268, fig. 252. Quebec. 
 
 [ Asaphiscus ] wheeleri. (See Asaphiscus wheeleri.) 
 
 Bathyuriscus Meek, 1873; 6th Ann. Rept. U. S. Geol. Survey Territories, p. 484. 
 
 [Bathyiirusf] haydeni Meek, 1873; 6th Ann. Rept. U. S. Geol. Survey Terri- 
 tories, p. 483. Potsdam. 
 
 haydeni Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 215. 
 
 howelli Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 216, pi. 30, figs. 2, 2 a. 
 
 Middle Cambrian. 
 
 Syn., Emholimus rotundatus (Rominger) Walcott, 1888; Am. Jour. Sci., 3d series, 
 vol. 36, p. 165, referred to Bathyuriscus howelli. 
 
 LOgygia~\ producta Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par., vol. 
 
 4, p. 244, pi. 2, figs. 31-34. Middle Cambrian. 
 
 VOgyyia'] producta Hall and Whitfield, 1877; U. S. Geol. Expl. 40th Par., vol. 
 
 4, p. 245, pi. 2, fig. 35. 
 
 producta Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 217, pi. 30, figs. 1, 
 
 1 a-c. 
 
 Bathyurus Billings, 1859 ; Canadian Naturalist, vol. 4, p. 364. 
 
 Type, Bathyurus extans Hall. 
 
 amplimarginatus Billings, 1857 ; Canadian Naturalist, vol. 4, p. 365, fig. 12 a, b. 
 
 Calciferous. 
 
 amplimarginatus Billings, 1863 ; Geol. Canada, p. 122, fig. 41. 
 
 amplimarginatus Billings, 1865; Pal. Foss., vol. 1, p. 352, fig. 341 a. 
 
 angelini Billings, 1859 ; Canadian Naturalist, vol. 4, p. 467, fig. 37. Chazy. 
 
 angelini Billings, 1863 ; Geol. Canada, p. 133, fig. 68. 
 
 arcuatus Billings, 1865; Pal. Foss., vol. 1, p. 205, fig. 190. Quebec. 
 
 armatus Billings, 1860 ; Canadian Naturalist, vol. 5, p. 319, fig. 23. 
 
 armatus Billings, 1865 ; Pal. Foss., vol. 1, p. 411, fig. 392. 
 
 armatus Walcott, 1879 ; 32d Rept. New York State Mus. Nat. Hist., p. 131. 
 
 [ Dorypyge? ] armatus Vogdes, Bull. U. S. Geol. Survey No. 63 (this bulletin). 
 
 bitub erculatus Billings, 1860; Canadian Naturalist, vol. 5, p. 319, fig. 22; also 
 
 Geol. Canada, 1863, p. 238, fig. 270. Quebec. 
 
 bituberculatus Billings, 1865; Pal. Foss., vol. 1, p. 410, fig. 391. 
 
 If this species is correctly represented by Mr. E. Billings it can not bo in- 
 cluded within the limits of Bathyurus. As we know of no other, to which it 
 bears a resemblance, the new generic term of Lloydia is proposed, in honor of 
 the first author on Trilobites, Edward Lliwyd. Diagnosis : Glabella tumid 
 and extending to the frontal limb ; basal lobes elongate-oval, pointed at both 
 ends, separated from the glabella by shallow, obscure grooves ; eyes opposite 
 the mid length of the glabella ; thorax unknown. 
 
 breviceps Billings, 1865; Pal. Foss., vol. 1, p. 262, fig. 246. Quebec. 
 
 capax Billings, 1860; Canadian Naturalist, vol. 5, p. 318, fig. 20. Quebec. 
 
 capax Billings, 1863; Geol. Canada, p. 238, fig. 271. 
 
 capax Billings, 1865; Pal. Foss., vol. 1, p. 409, fig. 389. 
 
 A similar species was referred by Mr. R. P. Whitfield (Geol. Survey Wiscon- 
 sin, vol. 4, pi. 4, fig. 6) to Dicelloccphalus. 
 
 caudatus Billings, 1865; Pal. Foss., vol. 1, p. 261, fig. 245. Quebec. 
 
 conicua Billiugs, 1859; Canadian Naturalist, vol. 4, p. 366, fig. 12 d. Calciferous. 
 
 conicua Billings, 1863; Geol. Canada, p. 122, fig. 42. 
 
 conicua Billings, 1865 ; Pal. Foss., vol. 1, p. 352, fig. 341 b. 
 
 conicua Whitfield, 1889 ; Bull. Am. Mus. Nat. Hist., vol. 2, No. 2, p. 61, pi. 13, 
 
 figs. 15-21. 
 
 Bull. 63 7 
 
98 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63 . 
 
 Bathyurus ? congeneris Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, 
 vol. 8, p. 92, pi. 12, fig. 8. Pogonip. 
 
 cordai Billings, 1860 ; Canadian Naturalist, vol. 5, p. 321, fig. 26. Calciferous. 
 
 cordai Billings, 1863 ; Geol. Canada, p. 238, fig. 269. 
 
 cordai Billings, 1865 ; Pal. Foss., vol. 1, p. 259, fig. 242; p. 412, fig. 395. 
 
 Compare this species with typical Solenopleura. 
 
 ? crotalifrons Dwight, 1884; Am. Jour. Sci., 3d series, vol. 27, p. 253, figs. 4, 
 
 4 a, 5, 6. Calciferous. 
 
 cybele Billings, 1859 ; Canadian Naturalist, vol. 4, p. 366, fig. 12 c. Calciferous. 
 
 cybele Billings, 1863 ; Geol. Canada, p. 122, fig. 43. 
 
 cybele Billings, 1865; Pal. Foss., vol. 1, p. 352, fig. 341c. 
 
 dubius Billings, 1860 ; Canadian Naturalist, vol. 5, p. 319, fig. 21. Quebec. 
 
 dubius Billings, 1865; Pal. Foss., vol. 1, p. 410, fig. 390. 
 
 [ Asaphus? ] extans Hall, 1847; Pal. New York, vol. 1, p. 228, pi. 60, figs. 2a-c. 
 
 Trenton. 
 
 [ Asaphus f ] extans Hall, 1850 ; 3d Rept. New York State Cab. Nat. Hist., p. 174, 
 
 pi. 3, figs. 1 a-c. 
 
 Syn., Asaphus nodosiriatus Hall, 1850 ; 3d Rept. New York State Cab. Nat. Hist., 
 p. 175. 
 
 extans Billings, 1863; Geol. Canada, p. 153, fig. 114. 
 
 gregarius Billings, 1865 ; Pal. Foss., vol. 1, p. 363, fig. 349. Potsdam. 
 
 Mr. Walcott (Bull. U. S. Geol. Survey, No. 10, p. 36) refers this species to 
 the genus Solenopleura Angelin, and remarks that many of the Cambrian species 
 of the genus Bathy urus described in the Canadian reports might be referred to 
 that genus? 
 
 ? haydeni. (See Bathyuriscus haydeni.) 
 
 longispinus Walcott, 1876 ; 28th Rept. N. Y. State Cab. Nat. Hist., p. 94. 
 
 Trenton. 
 
 minganensis Billings, 1865 ; Pal. Foss., vol. 1, p. 353. Calciferous. 
 
 nero. (See Solenopleura nero (Billings) Walcott.) 
 
 oblongus Billings, 1860 ; Canadian Naturalist, vol. 5, p. 321, fig. 25. Quebec. 
 
 oblongus Billings, 1865; Pal. Foss., vol. 1, p. 412, fig. 394. 
 
 parvulus Billings, 1861; Geol. Vermont, vol. 2, p. 952, fig. 361. 
 
 parvulus Billings, 1861 ; Pal. Foss., Bull. Geol. Sur. Canada p. 16, fig. 21. 
 
 Potsdam. 
 
 parvulus Billings, 1865 ; Pal. Foss., vol. 1, p. 16, fig. 21. 
 
 perplexus Billings, 1865; Pal. Foss., vol. 1, p. 364, fig. 350. Potsdam. 
 
 perspicator Billings, 1865; Pal. Foss., vol. 1, p. 205, fig. 191. Quebec. 
 
 pogonipensis Hall and Whitfield, 1877; U. S. Geol. Expl. 40th Par., vol. 4, p. 
 
 243, pi. 1, figs. 33, 34. Cambrian. 
 
 quadratus Billings, 1860; Canadian Naturalist, vol. 5, p. 321, fig. 27. Quebec. 
 
 quadratus Billings, 1865 ; Pal. Foss., vol. 1, p. 412, fig. 396. 
 
 saffordi Billings, 1860 ; Canadian Naturalist, vol. 5, p. 321, fig. 24. Quebec. 
 
 saffordi Billings, 1865 ; Pal. Foss., vol. 1, p. 259, fig. 341 ; p. 411, fig. 393. 
 
 seelyi Whitfield, 1886 ; Bull. Am. Mus. Nat. Hist., New York, vol. 1, No. 8, p. 339, 
 
 pi. 33, figs. 12-18. Birdseye. 
 
 seelyi Whitfield, 1889 ; Bull. Am. Mus. Nat. Hist. , New York, vol. 2, No. 2, p. 62, 
 
 pi. 13, figs. 8-14. 
 
 senectus Billings, 1861 ; Bull. Geol. Sur. Canada, p. 16. Potsdam. 
 
 senectus Billings, 1861 ; Geol. Vermont, vol. 2, p. 953, figs. 359, 360. 
 
 senectus Billings, 1863 ; Geol. Canada, p. 286, figs. 298 a, b ; Pal. Foss., vol. 1. p. 
 
 16 (1865), figs. 19,20. 
 
 Referred to Protypus senectus Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, 
 p. 213, pi. 31, figs. 2, 2 a-c. 
 
VOGDBS. ] 
 
 CATALOGUE OF TRILOBITES. 
 
 99 
 
 Bathyurus serratus Meek, 1873; 6th Ann. Kept. U. S. Geol. Survey Territories, p. 
 480. Potsdam. 
 
 ? simillimus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 93, pi. 12, fig. 11. Pogonip. 
 
 smithi Billings, 1863; Geol. Canada, p. 153, fig. 115. Trenton. 
 
 smithi Billings, 1865 ; Pal. Foss., vol. 1, p. 56. 
 
 solitaricus Billings, 1865 ; Pal. Foss., vol. I,j9. 362. Quebec. 
 
 [^cidaspis] spiniger Hall, 1847 ; Pal. New York, vol. 1, p. 241, pi. 64, fig. 5. 
 
 Trenton. 
 
 stonemani Yogdes, 1884 ; 12th Ann. Kept. Geol. Nat. Hist. Minnesota, p. 8. 
 
 Trenton. 
 
 strenuus Billings, 1865; Pal. Foss., vol. 1, p.204, fig. 188. Quebec. 
 
 taurifrons Dwight, 1884 ; Am. Jour. Sci., 3d series, vol. 27, p. 252, pi. 7, figs. 1-3. 
 
 Calciferous. 
 
 timon Billings, 1865 ; Pal. Foss., vol. 1, p. 261, fig. 244. Quebec. 
 
 ? tuberculatus Walcott, 1884 ; Pal. Eureka Diet., Mon. U. S. Geol. Survey, vol. 
 
 8, p. 12, fig. 9. Pogonip. 
 
 vetula Billings, 1865; PaT. Foss., vol. 1, p. 365. ^ Potsdam. 
 
 [ Agraulos ( Batliym'us?) ] woosteri Whitfield, 1878; Ann. Rept. Geol. Survey 
 
 Wisconsin, p. 56. Potsdam. 
 
 [ Agraulos {Bathyurus ?)] woosteri Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 
 
 189, pi. 1, figs. 19-21. 
 
 Bohemilla Batrande, 1872; Syst. Sil. Boheme, Suppl., vol. 1, p. 137. 
 
 Type, Bohemilla stupenda Barrande. 
 
 Brongniartia Eaton, Am. Jour. Sci., 1st series, vol. 22, p. 166, and Geol. Text-Book, p. 
 32 (Syn., Asaphus in part), not Brongniartia Salter (subgenus Homalonotus). 
 
 carcinoides Eaton. (See Triarthrus becki.) 
 
 isoletea. (See Asaphus platycephalus.) 
 
 platycephus Eaton. (See Homalonotus delphinocephalus.) 
 
 Brachymetopus McCoy, 1847; Ann. Nat. Hist., vol. 20, p. 220. 
 
 Type, Brachymetopus maccoyi Portlock. 
 
 \_Phillip8ia ( Griffithides )] lodiensis Meek, 1875; Pal. Ohio, vol. 2, p. 323, pi. 18, 
 
 fig. 3. Waverly. 
 
 lodiensis Yogdes, 1888; Annals New York Acad. Sci., vol. 4, p. 102. 
 
 [ Phillipsia ( Brachymetopus )] ornata Hall. (See Cyphaspis ornata.) 
 
 Bronteus Goldfuss, 1839; feeitrage Petrefactenkunde, Nova Acta Physico-Med., vol. 
 19, p. 360, pi. 33, fig. 3. 
 
 Type, Bronteus flahellif era Goldfuss. 
 
 Syn., Goldius De Koninck, 1841 ; M6m. Crust. Foss. Belgique, p. 5. 
 
 acamas Hall, 1865; 20th Rept. New York State Cab. Nat. Hist., p. 332, pi. 21, 
 
 figs. 19,20. Niagara. 
 
 acamas Hall, 1870; 20th Rept. New York State Cab. Nat. Hist., p. 422, pi. 21, 
 
 figs. 19, 20 (rev. ed.). 
 
 barrandi Hall, 1859; Pal. New York, vol. 3, p. 350, pi. 63, figs. 1-4. 
 
 Lower Helderberg. 
 
 canadensis Logan, 1844; Geol. Canada, p. 54, 2 figs. Lower Helderberg. 
 
 insularis Billings, I860; Catalogue Sil. Foss. Anticosti, p. 66. 
 
 laphami Whitfield, 1878; Ann. Rept. Geol. Survey Wisconsin (1877), p. 88. 
 
 Niagara. 
 
 laphami Whitfield, 1882 ; Geol. Wisconsin, vol. 4, p. 310, pi. 22, figs. 1-4. 
 
 lunatus Billings, 1857; Geol. Canada, p. 338. Trenton. 
 
 lunatus Billings, 1863; Geol. Canada, p. 188, fig. 187. 
 
 ? niagarensis Hall, 1852; Pal. Now York, vol. 3, p. 314, pi. 70, fig. 3. 
 
 Niagara. 
 
100 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA, 
 
 [BULL. 63 . 
 
 Bronteus occasus Winehell and Marey, 1866; Mem. Boston Soc. Nat. Hist., vol. 1, 
 p. 104, pi. 3, fig. 12. Niagara. 
 
 occasus (Winehell and Marey) Hall, 1867 ; 20th Rept. New York State Cab. Nat. 
 
 Hist., p. 400. 
 
 pompilius Billings, 1863; Proc. Portland Soc. Nat. Hist., p. 123, pi. 1, fig. 25. 
 
 Upper Silurian. 
 
 tullius Hall, 1888; Pal. New York, vol. 7, p. 12, pi. 8, figs. 34-36. Hamilton. 
 
 Bumastus Murchison, 1839 ; Sil. Syst., p. 656. Subgenus, Illcenus. 
 
 Calymene Brongniart, 1822 ; Crust. Fos., p. 9. 
 
 Type, Calymene tuberculata Biinnich, 1781. 
 
 Syn., Prionocheilus, Rouault, Bull. Soc. G6ol. France, vol. 4, 1846, p. 309. 
 
 anchiops. (See Dalmanites anchiops.) 
 
 beckii. (See Triarthrus becki.) 
 
 blumenbachi Brongniart, 1822; Crust. Foss., p. 11, pi. 1, figs. 1 a-d. 
 
 ■ blumenbachi Barrande, 1852; Syst. Sil. Boherne, pis. 19 and 45. 
 
 blumenbachi Salter, 1863; Mon. Brit. Trilobites, pi. 8, figs. 7-11, 13-16; pi. 9, 
 
 fig. 1. 
 
 This species should take the older name of Calymene tuberculata Biinnich. 
 
 blumenbachi (Green) not Brong., Mon. Tril. N. A., p. 28, cast 1. 
 
 blumenbachi ? Foerste, 1885 ; Bull. Denison Univ., vol. 1, p. 100, pi. 13, fig. 25. 
 
 bucklandi. (See Ceraurus pleurexanthus Green.) 
 
 bufo. (See Fhacops bufo Green.) 
 
 bufo var. rana. (See Phacops rana Green.) 
 
 callicephala Green, 1832; Mon. Tril. N. A., p. 30, cast 2. 
 
 callicephala'Burmeister, 1843 ; Org. Trilobiten, p. 83, pi. 2, figs. 9-10 (Ray Soc. 
 
 ed.). 
 
 callicephala Miller, 1882 ; Jour. Cincinnati Soc. Nat. Hist., vol. 5, p. 117, pi. 5, 
 
 fig. 8. 
 
 The cast of this species (from a dark yellowish limestone of Hampshire 
 County, Virginia), issued with Dr. Green’s monograph, exhibits a Calymene 
 with a broad frontal margin. The other specimens referred to by Dr. Green 
 from Ohio and Indiana are species of the well-known Calymene senaria Conrad. 
 
 camerata Conrad, 1842; Jour. Acad. Nat. Sci. Phila., vol. 8, p. 278. Niagara. 
 
 camerata Hall, 1852; Pal. New York, vol. 2, p. 337, pi. 78, figs. 10 a-f. 
 
 christyi Hall, 1860; 13th Rept. New York State Cab. Nat. Hist., p. 119. 
 
 Hudson. 
 
 christyi Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., pi. 10, figs. 1,2, 
 
 and 5. 
 
 • christyi Hall and Whitfield, 1875 ; Pal. Ohio, vol. 2, p. 107, pi. 4, figs. 13-15. 
 
 christyi Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 141. 
 
 [ Hemicrypturis ] clintoni Vanuxem, 1842; Geol. New York, 3d Geol. Dist., p. 79, 
 
 fig. 3; also p. 80. Clinton. 
 
 clintoni Hall, 1852; Pal. New York, vol. 2, p. 298, pi. 66 a, figs. 5 a-d. 
 
 clintoni Rogers, 1858 ; Geol. Survey Pennsylvania, vol. 2, p. 823, fig. 637. 
 
 clintoni Vogdes, 1880; Proc. Acad. Nat. Sci. Phila., p. 178, figs. 3,4 (not fig. 3). 
 
 clintoni Vogdes, 1886; Des. New Species Foss. Crust. Clinton Group, p. 5, figs. 3, 4. 
 
 (See Calymene vogdesii Foerste.) 
 
 conradi Emmons, 1855; Am. Geology, vol. 1, pt. 2, p. 236. Hudson. 
 
 crassimarginata. (See Proetus crassimarginata.) 
 
 diops Green, 1832 ; Mon. Tril. N. A., p. 37, pi. 1, fig. 2, cast 8 ( Proetus diops). • 
 
 macrophthalma Green, 1832 ; Mon. Tril. N. A., p. 39, cast 9. (See Phacops bufo. ) 
 
 mamillata Hall, 1861 ; Geol. Wisconsin, p. 50. Trenton. 
 
 mamillata Hall, 1862; Geol. Wisconsin, vol. 1, p. 432, figs. 1,2. 
 
 marginatus. (See Proetus marginatus.) 
 
V0GDE8. 1 
 
 CATALOGUE OF TRILOBITES. 
 
 101 
 
 Calymene microps Green, 1832; Mon. Tr.il. N. A., p. 34, cast 6. 
 
 multicosta Hall, 1847 ; Pal. New York, vol. l,p. 228, pi. 60, fig. 3. Trenton. 
 
 nasuta Ulrich, 1879; Jour. Cincinnati Soc. Nat. Hist., vol. 2, p. 131, fig. 3. 
 
 Niagara. 
 
 niagarensis Hall, 1843; Geol. New York, 4th Dist., p. 102, fig. 3 (on p. 101). 
 
 Niagara. 
 
 blumenbachii var. niagarensis Hall, 1852 ; Pal. New York, vol. 2, p. 307, pi. 67, 
 
 figs. 11, 12. 
 
 blumenbachii Roemer, 1860; Sil. Fauna W. Tenn., p. 79, pi. 5, fig. 22. 
 
 niagarensis Hall and Whitfield, 1875 ; Pal. Ohio, vol. 2, p. 153, pi. 7, figs. 14, 15. 
 
 niagarensis Hall; 20th Rept. New York State Cab. Nat. Hist., p. 334 ; revised 
 
 edition, p. 425. 
 
 niagarensis Hall, 1876; Illus. Devon. Foss. Crustacea, pi. 1, fig. 10. 
 
 niagarensis Hall, 1879 ; 28th Rept. N. Y. State Mus. Nat. Hist., p. 187, pi. 32, figs. 
 
 8-15. 
 
 niagarensis Hall, 1883; 11th Ann. Rept. Geol. Nat. Hist. Indiana, 1881, p. 331. 
 
 pi. 34, figs. 8-15. 
 
 Compare C. brevicapitata (Portlock) McCoy; Brit. Pal. Foss., pi. 1 F, fig. 4. 
 
 nupera. (See Phacops nupera.) 
 
 odontocephala. (Syn., Dalmanites selenus.) 
 
 phlyctainodes Green, 1837 ; Am. Jour. Sci., 1st series, vol. 32, p. 167. 
 
 Dr. Green compares this species with Encrinurus variolaris. 
 
 platys Green, 1832; Mon. Tril. N. A., p. 32, casts 4,5. Upper Helderberg. 
 
 platys Hall, 1861 ; Des. New Species Foss., p. 54. 
 
 platys Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 82. 
 
 platys Hall, 1876 ; Illus. Devon. Foss. Crustacea, pi. 1, figs. 1-9. 
 
 platys Hall, 1888; Pal. New York, vol. 7, p. 1, pi. 1, figs. 1-9; pi. 25, figs. 
 
 1 , 2 . 
 
 rana. (See Phacops rana Green.) 
 
 rostrata Yogdes, 1879; Am. Jour. Sci., 3d series, vol. 18, p. 477. . Clinton. 
 
 rostrata Vogdes, 1880; Proc. Acad. Nat. Sci. Phila., p. 176, figs. 1,2. 
 
 rostrata Yogdes, 1886; Des. New Species Foss. Crust. Clinton Group, p. 2, figs. 
 
 1 , 2 . 
 
 rowi. (See Phacops rowi Green.) 
 
 - — rugosa Shumard, 1855; 1st and 2d Repts. Geol. Missouri, p. 200, pi. B, fig. 14. 
 
 Lower Helderberg. 
 
 selenecephala. (See Calymene senaria Conrad.) 
 
 senaria Conrad, 1841; 4th Ann. Rept. Pal. Dept. New York Geol. Survey, p. 49. 
 
 Trenton. 
 
 senaria Emmons, 1842; Geol. New York, 2d Geol. Dist., p. 390, fig. 2. 
 
 Syn., selenecephala Green, 1832 ; Mon. Tril. N. A., p. 31, cast 3. 
 
 blumenbachii Green, 1832; Mon. Tril. N. A., p. 28, cast 1. (Not of Bron- 
 gniart.) 
 
 callicephala Green, 1832; Mon. Tril. N. A., p. 31. (Specimens from Ohio 
 and Indiana only.) 
 
 brevicapitata Salter, 1848 ; Mem. Geol. Surv. United Kingdom, vol. 2, p. 341, 
 pi. 11, figs. 1, 2. (Not of Portlock, 1843 ; Geol. Rept. Londonderry, etc., 
 p. 286, pi. 3; fig. 3.) 
 
 brevicapitata (Portlock) Salter; Mem. Geol. Surv. United Kingdom, vol. 3, 
 pi. 17, figs. 11, 12. (Not of Portlock.) 
 forcipata (McCoy) Salter; Palaeon. Soc. London, vol. 17, p. 97. (Not of 
 McCoy, Sil. Foss. Ireland, pi. 4, fig. 14.) 
 
 senaria Emmons, 1855; Am. Geology, vol. 1, pt. 2, p. 213, pi. 16, fig. 9. 
 
 senaria Hall, 1847 ; Pal. New York, vol. 1, p. 238, pi. 64, figs. 3 a-n. 
 
[BULL. 63 . 
 
 102 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Calymene \bhinienbachii] var. senaria Hall, 1852; Pal. New York, vol. 2, p. 290, pi. 
 66 a, tigs. 6 a-e. Clinton. 
 
 senaria var. blumenbachii Salter, 1865; Mon. Brit. Tril., p. 97, pi. 9, figs. 6-10 (not 
 
 figs. 7, 8, Calymene brevicapitata Portlock). 
 
 senaria Meek, Pal. Ohio, vol. 1, p. 173, pi. 14, figs. 14 a-f. 
 
 senaria Miller, 1874; Cincinnati Quart. Jour. Sci., vol. 1, p. 140. 
 
 Syn., calhcephala (Green) Miller, 1877 ; Catalogue Am. Pal. Foss., p. 213. 
 
 senaria White, 1880; 2d Ann. Rept. Dept. Statistics Geol. Indiana, p. 493, pi. 2, 
 
 figs. 1,2. 
 
 Syn., callicephala (Green) Miller, 1882; Jour. Cincinnati Soc. Nat. Hist., vol. 5, 
 p. 117, pi. 5, fig. 8. 
 
 senaria Walcott, 1887 ; Notes on Some Sections of Trilobites, pi. 1. 
 
 senaria Walcott, 1884 ; Science, March 7, 1884, vol. 3, p. 201, figs. 2, 3. 
 
 spinifera Conrad, 1842; Jour. Acad. Nat. Sci. Phila., vol. 8, p. 277. 
 
 Compare Cyphaspis girardeauensis. 
 
 trisulcata. (See Phacops trisulcata.) 
 
 vogdesii Foerste, 1887; Bull. Denison Univ., vol. 2, p. 95, pi. 8, figs. 12-16. 
 
 Clinton. 
 
 ? blumenbachi Foerste, 1886 ; Bull. Denison Univ., vol. 1, p. 190, pi. 13, fig. 24. 
 
 Syn., clintoni Yogdes, 1882 ; Proc. Acad. Nat. Sci. Phila., p. 178, fig. 3 (not fig. 4). 
 clintoni Yogdes, 1886; Des. New Species Foss. Crust. Clinton Group, p. 5, 
 fig. 3 (not fig. 4). 
 
 Ceratocephala Warder, 1838. (See Acidaspis.) 
 
 ceralepta Anthony. (See Acidaspis ceralepta.) 
 
 goniata Warder, 1838; Am. Jour. Sc., 1st series, vol. 34, p. 378, figure. 
 
 Ceratolichas Hall, 1888 ; Pal. New York, vol. 7, p. xl. Subgenus Lichas. 
 
 Ceraurus Green, 1832; Monthly Am. Jour. Geol., vol. 1, p. 560, pi., fig. 6; Mon. Tril. 
 
 N. A., p. 83, cast 33, pi., fig. 10. 
 
 Ceraurus Hall, 1847; Pal. New York, vol. 1, p. 242. 
 
 Syn., Otarion (in part) Zenker, 1833 ; Beitrage Nat. Urwelt, p. 44. 
 
 Arges (in part) Goldfuss, 1843; Neues Jahrbuch fur Mineral., p. 5. 
 Cyphaspis (in part) Burmeister, 1843, Org. Trilobiten, p. 104. 
 
 Amphion (in part) Portlock, 1843; Geol. Survey Londonderry, etc., p. 272. 
 Cyphaspis (in part) McCoy, 1846 ; Sil. Foss. Ireland, p. 44. 
 
 Cheirurus Beyrich, 1846 ; Unters. Trilobiten, etc. II, p. 3. 
 
 Eccoptochile Corda, 1847 ; Prodr., p. 245. 
 
 Actinopeltes Corda, 1847 ; Prodr., p. 247. 
 
 Crotalocephalus Salter, 1853 ; Mem. Geol. Survey United Kingdom, decade 
 7, pi. 2, p. 10. 
 
 Cyrtometopus Angelin, 1854; Pal. Scand., p. 32. 
 
 Sphcerocoryphe Angelin, 1854; Pal. Scand., p. 65. 
 
 Pseudophceroxochus Schmidt, 1881; Rev. Baltic Sil. Tril., p. 130. 
 Nieszkowskia Schmidt, 1881 ; Rev. Baltic Sil. Tril., p. 130. 
 
 Type, Ceraurus pleurexanthemus Green. 
 
 ICheirurus ] appollo Billings, 1860; Canadian Naturalist, vol. 5, p. 322, fig. 28. 
 
 Quebec. 
 
 [Cheirurus'] appollo Billings, 1865; Pal. Foss., vol. 1, p. 413, fig. 397. 
 
 [Cheirurus ] bimucronatus (Murch.) Roemer, Die sil. Fauna W. Tenn., p. 80, pi. 5, 
 
 fig. 19, not of Murchison. (See Ceraurus niagarensis Hall.) 
 
 crosotus Lock. (See Acidaspis crosotus.) 
 
 [Cheirurus] eryx Billiugs, 1860 ; Canadian Naturalist, vol. 5, p. 322, fig. 30. 
 
 Quebec. 
 
 [Cheirurus] eryx Billings, 1865; Pal. Foss., vol. 1, p. 413, fig. 399. 
 
 [Cheirurus] glaucus Billings, 1865 ; Pal. Foss., vol. 1, p. 323, fig. 308. Quebec. 
 
VODGES.] 
 
 CATALOGUE OF TRILOBITES. 
 
 103 
 
 Ceranrus [Cheirurus} icarus Billings, 1860 ; Canadian Naturalist, vol. 5, p. 67, fig. 14. 
 
 Hudson. 
 
 [Cheirurus} icarus Billings, 1863; Geol. Canada, p. 219, fig. 231. 
 
 icarus Meek, 1873 ; Pal. Ohio, vol. 1, p. 162, pi. 14, fig. 11 a, b, c. 
 
 icarus Miller, 1874; Cincinnati Quart. Jour. Sci.,vol. l,p. 133. 
 
 [Cheirurus} insignis (Beyrich) Hall, 1852; Pal. New York, vol. 2, p. 300, also 
 
 p. 306, pi. 67, figs. 9, 10. 
 
 Not of Beyrich, 1845; Ueber einige bohm. Tril., p. 12, pi. 1, fig. 1, 
 
 insignis. (See Ceraurus niagarensis Hall.) 
 
 mercurius Billings, 1865; Pal. Foss., vol. 1, p. 285, fig. 272. Quebec. 
 
 niagarensis Hall, 1867 ; 20tb Kept. New York Stale Cab. Nat. Hist., p. 376, pi. 
 
 21, fig. 10. 
 
 niagarensis Hall, 1870; 20th Rept. New York State Cab. Nat. Hist. (2d ed.), p. 
 
 427, pi. 21, figs. 10, 11. 
 
 Syn., Sphcerexochus romingeri ? Hall ; Doc. Ed. 2Sfch Rept. New York State Mus. 
 Nat. Hist. 
 
 Explanation of pi. 32, fig. 16 (erroneous reference). 
 
 [ Cheirurus ] niagarensis Hall, 1879 ; 28th Rept. New York State Mus. Nat. Hist., 
 
 p. 189, pi. 32, fig. 16. 
 
 Syn., Cheirurus bimucronatus (Murch.) Roerner ; Die sil. Fauna W. Tenn., p. 80, 
 pi. 5, fig. 19. 
 
 niagarensis Hall, 1882; 12th Ann. Rept. Geol. Nat. Hist. Indiaua, 1881, p. 335, 
 
 pi. 34, fig. 16; pi. 33, fig. 10. 
 
 [Cheirurus} numitor Billings, 1866 ; Catalogue Sil. Foss. Anticosti, p. 27, fig. 11. 
 
 Hudson. 
 
 [ Cheirurus ] nuperus Billings, 1866; Catalogue Sil. Foss. Anticosti, p. 61, fig. 20. 
 
 Anticosti. 
 
 [Cheirurus} perforator Billings, 1865; Pal. Foss., vol. 1, p. 287, fig. 275. 
 
 Quebec. 
 
 pleurexanthemus Green, 1832; Monthly Am. Jour. Geol., vol. 1, p. 560, pi., 
 
 fig. 10. Trenton and Hudson. 
 
 pleurexanthemus Green, 1832; Mon. Tril. N. A., p. 84, fig. 10, pi. 1, cast 33. 
 
 Syn., Calymene bucklandi Anthony, 1838; Am. Jour. Sci., 1st series, vol. 36, p. 
 106, figs. 1, 2. 
 
 pleurexanthemus Hall, 1847 ; Pal. New York, vol. 1, p. 242, pi. 65, figs. 1 a-n ; 
 
 pi. 66, figs. 1, 1 h. 
 
 pleurexanthemus Emmons, 1855 ; Am. Geology, vol. 1, p. 217, pi. 15, figs. 1 a-k. 
 
 [ Cheirurus ] pleurexanthemus Billings, 1863; Geol. Canada, p. 188, fig. 188. 
 
 pleurexanthemus Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 132. 
 
 pleurexanthemus Walcott, 1875; Annals Nat. Hist. New York, vol. 11, p. 155, 
 
 pi. 11. 
 
 pleurexanthemus Walcott, 1881 ; Bull. Mus. Comp. Zool. Harvard Coll., vol. 
 
 8, p. 211, pi. 5, figs. 1-6. 
 
 [ Cheirurus} polydorus Billings, 1865 ; Pal. Foss., vol. 1, p. 286, fig. 274. Quebec. 
 
 [Cheirurus} pompilius Billings, 1865 ; Pal. Foss., vol. 1, p. 181, fig. 162. 
 
 Chazy and Hudson. 
 
 [ Cheirurus} prolificus Billings, 1865 ; Pal. Foss., vol. 1, p. 285, fig. 273 ; p. 325, fig. 
 
 311. Quebec. 
 
 ? pustulosa Hall, 1847 ; Pal. New York, vol. 1, p. 246, pi. 61, fig. 2 a-li. 
 
 Trenton. 
 
 rarus Walcott, 1877 ; Advanced sheets 31st Rept. Now York State Mus. Nat. 
 
 Hist., p. 15. Trenton. 
 
 rarus Walcott, 1879^ 31st Rept. New York State Mus. Nat. Hist., p. 68. 
 
 [Cheirurus} satyrus Billings, 1865 ; Pal. Foss., vol. 1 , p. 324, fig. 309. Chazy. 
 
104 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63 . 
 
 Ceraunis [ Cheirurus ] sol Billings, 1865 ; Pal. Foss., vol. 1, p. 288, fig. 276. Quebec. 
 
 [ Cheirurus ] solitarius Billings, 1865 ; Pal. Foss., vol. 1, p. 206. . Quebec. 
 
 [ Cheirurus ] tarquinius Billings, 1863; Proc. Portland Soc. Nat. Hist., vol. 1, p. 
 
 121, pi. 1, fig. 22. Upper Silurian. 
 
 vigilans. (See Encrinurus vigilans.) 
 
 [ Cheirurus ] vulcanus Billings, 1865; Pal. Foss., vol. 1, p. 284, fig. 27; p. 324, 
 
 fig. 310. Quebec. 
 
 Chariocephalus Hall, 1863 ; 16th Rept. New York State Cab. Nat. Hist., p. 175. 
 
 Type, Chariocephalus ivhitjieldi Hall. 
 
 tumifrons Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par., vol. 4, p. 224, pi. 
 
 2, figs. 38, 39. Potsdam. 
 
 ? tumifrons Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 61, pi. 10, fig. 16. 
 
 whitfieldi Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 175, pi. 6, 
 
 figs. 49-53 ; pi. 10, fig. 20. Potsdam. 
 
 Chasmops McCoy, 1849; Annals Mag. Nat. Hist., 2d series, vol. 4, p. 403. (See Dal- 
 manites [ Chasmops ] anchiops, anchiops var. armatus, anchiops var. sobri- 
 nus, D. [ Chasmops ] calypso, D. [Chasmops'] erina, D. [ Chasmops ] macrops. 
 
 [ Dahnanites ] troosti Safford, 1869: Geol. Tennessee, p. 290. Trenton. 
 
 troosti Safford and Vogdes, 1889; Proc. Acad. Nat. Sci. Phila., p. 167, figure. 
 
 Conoceplialus Zenker, 1833; Beitrage Nat. Urvvelt, p. 48. 
 
 Conocephalites Barrande, 1852; Syst. Sil. Boheme, vol. 1, p. 415. 
 
 For species previously classed under these genera, see Conocoryphe, Fty- 
 choparia, and Crepicephalus. 
 
 Conocoryphe C<irda, 1847 ; Prodr., p. 139, pi. 2, fig. 10. 
 
 Type, Conocoryphe sulzeri Schlotheim. 
 
 [Conocephalites] baileyi Hartt, 1868 ; Acadian Geology, p. 645 (3d ed.). St. John. 
 
 baileyi Matthew, 1884 ; Trans. Royal Soc. Canada, vol. 1, p. Ill, pi. 1, figs. 22-27. 
 
 [Bailiella] baileyi Matthew, 1884 ; Traus. Royal Soc. Canada, vol. 1, pi. 1, fig. 22. 
 
 [Salteria] baileyi Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 32, pi. 4, 
 
 figs. 3, 3 a ; pi. 5, figs. 7, 7 a. 
 
 The author herein proposed the subgenus Salteria (corrected to Bailiella) for 
 Erinnys Salter, a preoccupied generic name ; the same is true of Salteria, used 
 for a genus of fossil Crustacea. 
 
 [Conocephalites] calcifera Walcott, 1879; 32d Rept. New York State Mus. Nat. 
 
 Hist., p. 129. Calciferous. 
 
 [Conocephalites] cordillerae Rominger, 1887 ; Proc. Acad. Nat. Sci. Phila., p. 17, 
 
 pi. 1, fig. 7. Cambrian. 
 
 elegans Hartt, 1868; Acadian Geol. (3d ed.), p. 650. St.John. 
 
 elegans Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 33, pi. 4, figs. 2, 2 a, b. 
 
 gemini-spinosus Hartt. (See Conocoryphe matthewi.) 
 
 [Conocephalites] hartti Walcott, 1879 ; 32dRept. New York State Mus. Nat. Hist., 
 
 p. 131. Calciferous. 
 
 [Conocephalites] matthewi Hartt, 1868; Acadian Geology, p.646, fig. 224. 
 
 St. John. 
 
 [Conocephalites] matthewi Matthew, 1884; Trans. Royal Soc. Canada, vol. 1, p. 
 
 103, pi., figs. 6-21. 
 
 Syn., Harttia matthewi Walcott, 1884 ; Bull. U. S. Geol. Survey, No. 10, p. 19, pi. 
 1, fig. 3. 
 
 matthewi Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 28, pi. 4, figs.- 1, 
 
 1 a, b. 
 
 [Conocephalites] optatus Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., 
 
 p. 122, pi. 5 a, fig. 7. * Potsdam. 
 
 [Conocephalites] trilineatus. (See Atops trilineatus Emmons.) 
 
V0GDES.] 
 
 CATALOGUE OF TRILOBITES. 
 
 105 
 
 Conocoryphe [ Conocoryplie ] trilineatus. (See Atops trilineatus Emmons.) 
 
 — t— [Bailella J walcotti Matthew, 1884 ; Trans. Royal Soc. Canada, vol. 1, p. 119, pi. 
 1, figs. 36-36 b. St. John. 
 
 walcotti Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 30. 
 
 Conolichas Dames, 1877 ; Zeitschr. Deutseh. geol. Gesell., Berlin, 1877, p. 806. Cono- 
 lichas, subgenus Lidias Hall, 1888; Pal. New York, vol. 7, p. xxxix. 
 
 Coronura Hall, 1888 ; Pal. New York, vol. 7, p. xxxii. (See Dalmanties [ Coronura ] 
 aspectans, D. [Coronura'] myrmecophorus, and D. [ Coronura ] emargi- 
 natus.) 
 
 Corycephalus Hall, 1888 ; Pal. New York, vol 7, p. xxxiv. (See Dalmanites [ Cory - 
 eephalus ] regalis, D. [Cory eephalus] pygmaeus, and D. [Corycephalus] denta- 
 tus.) 
 
 Crepicephalus Owen, 1852; Rept. Geol. Survey Wisconsin, Iowa, and Minnesota, 
 p. 570. 
 
 There is hardly a question that Dr. D. D. Owen had before him when he 
 wrote the description of his genus Crepicephalus a true Ptychoparia. He re- 
 marks: “The rather flat, slipper-shaped glabella is tapering and slightly 
 acuminated anteriorly, with a faint ridge on the median line ; two small 
 and very superficial depressions and a posterior faint furrow very partially 
 divide the glabella. The facial sutures run nearly parallel to the margin of 
 the glabella and join a thickened, cord-like anterior narrow border, inclos- 
 ing a convex area, narrower in front than at the sides. Oblique plications 
 can sometimes be traced on the cheek-plate in advance of the eye, converg- 
 ing towards the apex of the glabella.” He refers the following figures to the 
 genus: Plate 1, fig. 8, Crepicephalus ?, pygidium from the Miniskah Trilobite 
 grit. Plate 1, fig. 13, Crepicephalus? wisconensis (n. s. ), part of cephalothorax 
 and a portion of the cephalic shield of D. granulosus ?. Plate 1 a, fig. 10, 
 glabella of Crepicephalus n. g., near Miniskah. Plate la, fig. 14, pygidium 
 of Crepicephalus? miniscaenis n. s., from Miniskah grits. Plate 1 a, fig. 16, 
 pygidium and portion of Crepicephalus (?) and portions of cephalothorax of 
 that genus, from the Miniskah Trilobite grit. Plate la, fig. 18, glabella of 
 Crepicephalus, near Miniskah, Mississippi River. 
 
 [ Bathyurus ?] angulatus Hall and Whitfield. (See Ptychoparia angulatus.) 
 
 [Loganellus] anyius Hall and Whitfield. (See Ptychoparia anytus.) 
 
 [Loganellus] centralis Whitfield. (See Ptychoparia oweni.) 
 
 gibbsi Whitfield, 1880 ; Ann. Rept. Geol. Survey Wisconsin, 1879, p. 50. 
 
 Potsdam. 
 
 gibbsi Whitfield, 1880 ; Geol. Wisconsin, vol. 2, p. 67. 
 
 gibbsi Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 184, pi. 10, figs. 12, 13. 
 
 [Loganellus] granulosa Hall and Whitfield. (Sec Ptychoparia granulosa.) 
 
 [Loganellus] haguei. (See Lisostracus haguei and Ptychoparia haguei. ) 
 
 [ Loganellus] maculosus Hall and Whitfield. (See Ptychoparia maculosus.) 
 
 [Loganellus] montanensis Whitfield. (See Ptychoparia montanensis.) 
 
 [Loganellus] nitidens Hall and Whitfield. (See Ptychoparia nitidens.) 
 
 onustus Whitfield, 1878; Ann. Rept. Geol. Survey Wisconsin, 1877, p. 53. 
 
 Potsdam. 
 
 onustus Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 182, pi. 1, figs. 22,23. 
 
 oweni. (See Agraulos oweni and Ptychoparia oweni.) 
 
 [Loganellus] planus Whitfield. (See Ptychoparia planus.) 
 
 [Loganellus] quadrans Hall and Whitfield. (See Ptychoparia quadrans.) 
 
 [Loganellus] simulator Hall and Whitfield. (See Ptychoparia nitidens.) 
 
 [Loganellus] unisulcatus Hall and Whitfield. (See Ptychoparia unisulcatus.) 
 
 ? wisconseneis Owen. (See Anomocare wisconsensis.) 
 
 Crepicephalus Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 35. 
 
 Type, Dikelocephalus ? io wen sis Owen. 
 
106 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63 . 
 
 Crepicephalus augusta Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 208, pi. 
 28,- figs. 2, 2 a, b. Middle Cambrian. 
 
 [ Dikelocephalus?] iowensis Oweu, 1852; Rept. Geol. Wisconsin, Iowa, and 
 
 Minnesota, p. 575, pi. 1, fig. 4 ; pi. 1 a, fig. 13. Potsdam. 
 
 Undetermined Trilobite Owen, 1848 ; Rept. Geol. Reconnoissance Chippewa 
 Land Dist., p. 14, pi. 7, fig. 1. 
 
 [ Conocephalites ] iowensis Shumard, 1863; Trans. Acad. Sci. St. Louis, vol. 2, 
 
 p. 102. 
 
 [Conocephalites] iowensis Hall, 1863; 16th Rept. New York State Cab. Nat. 
 
 Hist., p. 162, pi. 7, fig. 33; pi. 8, figs. 10-12 and 30. 
 
 iowensis Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 36. 
 
 iowensis Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 207. 
 
 liliana Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 209, pi. 28, figs. 3, 
 
 3 a, c. Middle Cambrian. 
 
 Cryphceus Green, 1837; Am. Jour. Sci., 1st series, vol. 32, p. 343. 
 
 Type, Cryphceus boothi Green. 
 
 [ Dalmanites ( Cryphceus )] barrisi Hall, 1888; Pal. New York, vol. 7, p. 48, pi. 16 a, 
 
 fig. 18. Hamilton. 
 
 boothi Green, 1837; Am. Jour. Sci., 1st series, vol. 32, p. 343, figure. Hamilton. 
 
 Syn., Cryphceus cjrceni Courad, 1839; 2d Ann. Rept. Pal. Dept. New York Geol. 
 Survey, p. 66. 
 
 Cryphceus calliieles Conrad, 1839 ; 2d Ann. Rept. Pal. Dept. New York Geol. 
 Survey, p. 62. 
 
 Asaphus lialli Conrad, 1840; 3d Ann. Rept. Pal. Dept. New York Geol. Sur- 
 vey, p. 204. 
 
 Cryphceus calliteles Hall, 1843; Geol. New York, pt. 4, p. 201. 
 
 Cryphceus calliteles De Verneuil, 1850; Bull. Soc. G6ol. France, 2d series, 
 vol. 7, p. 164, pi. 1, fig. 3. 
 
 Pliacops peclinatus F. A. Roemer, 1850; Beitriige zur Kenntn. Harzgeb., p. 
 62, pi. 9, fig. 27. 
 
 Dalmania calliteles Emmons, 1860; Manual Geology, p. 138, fig. 124 (7). 
 
 [ Dalmania ] boothi Hall, 1861 ; Des. New Species of Fossils, p. 63. 
 
 [Dalmania] boothi Hall, 1862 ; 15th Rept. NeAv York State Cab. Nat. Hist., p. 91. 
 
 [ Dalmanites ] boothi Hall, 1876; Ulus. Devonian Foss., pi. 16, figs. 1-6, 9-11, 
 
 13, 15, 16. 
 
 Syn., Cryphceus stellifer Kayser, 1878; Abhandl. geol. Specialkarte Pr., vol. 2, 
 pt. 4, p. 33, (in part). 
 
 Cryphceus laciniatus Kayser, 1878; idem., p. 34. 
 
 [ Dalmanites (Cryphceus)] boothi Hall, 1888; Pal. New York, vol. 7, p. 42, pi. 16, 
 
 figs. 1-4 ; pi. 16 a, figs. 3-8. 
 
 callitelus Green, 1837 ; Am. Jour. Sci., 1st series, vol. 32, p. 346. 
 
 Hamilton. 
 
 [ Dalmanites ] boothi Hall, 1876; Illus. Devonian Foss., pi. 16, figs. 7, 8, 12, 14. 
 
 (?) callitelus Kayser, 1878 ; Abhandl. geol. Specialkarte Pr., vol. 2, pt. 4, p. 32, 
 
 pi. 3, tig. 10. 
 
 [ Dalmanites ( Cryphceus )] boothi var. calliteles Hall and Clarke, 1888; Pal. 
 
 New York, vol. 7, p. 45, pi. 16, figs. 5-22 ; pi. 16 a, figs. 9-17. 
 
 [Dalmanites (Cryphceus)] comis Hall, 1888; Pal. New York, vol. 7, p. 41, pi. 
 
 16 a, fig. 1. Corniferous. 
 
 [Dalmania] pleione Hall, 1861 ; Des. New Species Fossils, p. 62. Hamilton. 
 
 [Dalmania] pleione Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., 
 
 p. 90. 
 
 [Dalmanites] pleione Hall, 1876; 111ns. Devonian Foss., pi. 16, fig. 17. 
 
 pleione Kayser, 1878; Abhandl. geol. Specialkarte Pr., vol. 2, pt. 4, p. 33. 
 
VOGDE8.] 
 
 CATALOGUE OF TRILOBITES. 
 
 107 
 
 Cryphaeus [ Dalmanites, (Cfyphrens)^ pleione Hall, 18.88; Pal. New York, voL 7, p. 
 41, pi. 16 a, tig. 2. 
 
 Cryptolithus Green, 1832; Mon. Tril. North America, p. 72. 
 
 This generic should replace that of Trinucleus Murch., 1839. 
 
 Cryptonymus Eichwald, 1825 ; Syn. to Jsaphus, Illcenus, and Niobe. 
 
 Cryptonymus Eichwald, 1840. (See Encrimirus.) 
 
 Cybele Loven, 1845; Svenska Yetensk. Akad. Forliandl., p. 110. 
 
 Type, Cybele bellatula Dalman. 
 
 punctata Hall. (See Encrinurus ornatus.) 
 
 Cyphaspis Burmeister, 1843; Org. Trilobiten, p. 98. 
 
 Type, Cyphaspis ceratopthahna Burmeister. 
 
 christyi Hall, 1863; Trans. Albany Inst.,vol. 4, p. 220. Niagara. 
 
 christyi Hall, 1875; 28th Rept. New York State Mus. Nat. Hist., pi. 32, figs. 5-7. 
 
 christyi Hall, 1879 ; 28th Rept. New York State Mus. Nat. Hist., p. 188, pi. 32, 
 
 figs. 5-7. 
 
 - — christyi White, 1880; 2d Ann. Rept. Dept. -Statistics and Geol. Indiana, p. 
 493, pi. 3, fig. 9. 
 
 christyi Hall, 1882 ; 11th Ann. Rept. Dept. Geol. Nat. Hist. Indiana, 1881, p. 333, 
 
 pi. 34, figs. 5-7. 
 
 coelebs Hall, 1888 ; Pal. New York, vol. 7, p. 151, pi. 24, fig. 1. 
 
 Lower Helderberg. 
 
 craspedota Hall, 1888 ; Pal. New York, vol. 7, p. 148, pi. 24, figs. 15-20. 
 
 Hamilton. 
 
 diadema Hall, 1888; Pal. New York, vol. 7,p. 144, pi. 24, fig. 13. 
 
 Upper Helderberg. 
 
 girardeauensis Shumard, 1855 ; 1st and 2d Rept. Geol. Missouri, p. 197, pi. B, 
 
 fig. 11 a, b. 
 
 girardeauensis Emmons, 1860 ; Manual Geology, p. 159, fig. 145 (2). 
 
 hybrida Hall, 1888; Pal. New York, vol. 7, p. 144, pi. 24, fig. 14. 
 
 Upper Helderberg. 
 
 [ Phillipsia ] laevis Hall, 1876; Illus. Devonian Foss., pi. 21, fig. 29. 
 
 laevis Hall, 1888; Pal. New York, vol. 7, p. 150, pi. 21, fig. 29. Chemung. 
 
 [ Phillipsia ] minuscula Hall, 1876; Illus. Devonian Foss., pi. 20, fig. 17. 
 
 Upper Helderberg. 
 
 minuscula Hall, 1888 ; Pal. New York, vol. 7, p. 140, pi. 20, fig. 17 ; pi. 24, figs. 7-12. 
 
 [Phillipsia? ( Brachymetopus?)~\ ornata Hall, 1876; Illus. Devonian Foss., pi. 21, 
 
 fig. 1. Hamilton. 
 
 Syn., Phillipsia coronata Miller, 1877; Catalogue Am. Pal. Foss., p. 221. 
 
 Phillipsia coronata? Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Sur- 
 vey, vol. 8, p. 211. 
 
 ornata Hall, 1888 ; Pal. New York, vol. 7, p. 145, pi. 21, fig. 1 ; pi. 24, fig. 21. 
 
 ornata var. baccata Hall, 1888; Pal. New York, vol. 7, p. 146, pi. 24, figs. 22,23. 
 
 stephanophora Hall, 1888 ; Pal. New York, vol. 7, p. 142, pi. 24, tigs. 2-6. 
 
 Upper Helderberg. 
 
 Dalmania Emmrich, 1844 ; Zur Naturgoschichto Trilobiten, p. 15. 
 
 This name having been used in 1830 for a genus of the Diptera, J. Barrande 
 suggested that of Dahnanites. 
 
 Dalmanites (Emmrich) Barrande, 1872; Syst. Sil. Boheuio, Suppl., vol. 1, p. 27. 
 Type, JJalmanites caudatus Biinnich. 
 
 Syn., Pleuracanlhus Milne-Ed wards, 1840; Crnst., vol. 3, p. 329. 
 
 Odontochilc Corda, 1847 ; Prodr., p. 208, pi. 5, lig. 56. 
 
 Ostcropyye Corda, 1847 ; Prodr., p. 241, pi. 6, fig. 66. 
 
 Metacanthus Corda, 1817; Prodr., p.212, pi. 6, fig. 67. 
 
 Chasmops McCoy, 1849; Annals Nat. Hist., 2d series, vol. 4. 
 
108 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63 
 
 s.yn., Cryphwus Green, 1837; Am. Jour. Sci., 1st series, vol. 32, p. 343. 
 
 Odontocephalus Conrad, 1840; 3d Kept. Pal. Dept, New York Geol. Survey 
 p. 204. J 
 
 Hausmavnia Hall, 1888 ; Pal. New York, vol. 7, p. xxxi. 
 
 Coronura Hall, 1888 ; Pal. New. York, vol. 7, p. xxxii. 
 
 Corycephalus Hall, 1888 ; Pal. New York, vol. 7, p. xxxiv. 
 
 Dalmanites [Asaphus ?] acantholeurus (Conrad) Hall, 1862; 15th Rept. New Yort 
 State Cab. Nat. Hist., p. 113. 
 
 [Asaphus S'] acantholeurus Conrad, 1841 ; 4th Rept. Pal. Dept. New York Geol 
 Survey p. 48. Onondaaa 
 
 acantholeurus Hall, 1876; Ulus. Devonian Foss. Crust., pi. 19, fig 14 
 
 [Dalmamtes] acantholeurus Hall, 1876; Ulus. Devonian Foss. Crust., pi 19 
 
 fig. 14. ’ ! 
 
 achates Billings, 1860 ; Canadian Naturalist, vol. 5, p. 63, fig. 9. Trenton 
 
 achates Billings, 1863; Geol. Canada, p. 187, fig. 186. 
 
 aegeria Hall, 1861 ; Des. New Species Fossils, p. 57. Upper Helderbero- 
 
 aegeria Hall, 1862 ; 15th Rept. New York State Cab. Nat. Hist., p. 85. 
 
 ■ aegeria Hall, 1876; Ulus. Devonian Foss. Crust., pi. 12, figs. 1,2,7. 
 aegeria Hall, 1876; Illus. Devonian Foss. Crust., p. 12, figs 3, 6, 8 (not figs 
 1, 2, 7). 
 
 [Odontocephalus] aegeria Meek and Worthen, 1868; Geol. Illinois vol 3 p 417 
 
 pi. 10, figs. 4 a, b, c. * 
 
 [ Odontocophalus ] aegeria Hall, 1888 ; Pal. New York, vol. 7, p. 53, pi. 11 b, figs 
 
 [ Calymene ] anchiops Green, 1832; Monthly Am. Jour. Geol., vol. 1, p. 558. 
 
 r _ 7 Upper Helderberg. 
 
 [ Calymene ] anchiops Green, 1832; Mon. Tril. N. A., p. 35, cast 7. 
 
 Syn., Asaphus lalicostatus Green, 1832; Monthly Am. Jour. Geol., vol. 1, p. 559, 
 Asaphus laticostatus Green, 1832; Mon. Tril. N. A., p. 45, cast 13. * 
 
 [Phacops] anchiops Burmeister, 1843 ; Org. Trilobiten, p. 90 (Ray Soc. edition) 
 
 [Phacops] anchiops Hall, 1851; Rept. Geol. Lake Superior Land Dist. (Foster 
 
 and Whitney), pt. 2, p. 224, pi. 35, figs. 3 a, 3 b. (See Dalmanites anchiops 
 var. armatus.) 
 
 [DalmanW] anchiops Hal], 1861 ; Des. New Species Fossils, p. 55. 
 
 IDalmanm-] anchiops Hall, 1862; 15th Rept. New York State Cab. Nat. Hist. 
 
 p. 83. 
 
 anchiops Hall, 1876; Ulus. Devonian Foss. Crust., p. 9, fio-g. 1 3_6 9 10 12 
 13 ; pi. 10, figs. 6-14. 
 
 [Chasmops] anchiops Hall, 1888; Pal. New York, vol. 7, p.- 59 pi 9 fio-s 1-6 
 
 10, 12, 13; pi. 10, figs. 1-14. * * ' - 
 
 [Dalmania] anchiops var. armatus Hall, 1861 ; Des. New Species Foss., p. 56. 
 
 [Dalmania] anchiops var. armatus Hall, 1862; 15th Rept. New York State 
 
 Cab. Nat. Hist., p. 84. 
 
 anchiops var. armatus Hall, 1876; Illus. Devonian Foss. Crust., pi. 9, figs. 2, 
 
 7, 8. 
 
 [Chasmops] anchiops var. armatus Hall, 1888; Pal. New York, vol 7 p 62 nl 
 
 9, figs. 7-9; pi. 10, fig. 14. ' ’ P * 
 
 [Chasmops] anchiops var. sobrinus Hall, 1888; Pal. New York, vol. 17, p 62 
 
 pi. 9, fig. 11. f f ) 
 
 [Odontocephalus] arenarius Meek and Worthen, 1868 ; Geol. Survey Illinois, vol. 
 
 3, p. 417, pi. 9, fig. 10. (See Dalmanites selenurus.) 
 
 [Asaphus] aspectans Conrad, 1841; 5th Ann. Rept, Pal. Dept. New York Geol 
 
 Survey, p. 48, fig. 9. Upper Helderberg. 
 
 Syn., Asaphus? denticulatus Conrad; idem., p. 48. 
 
CATALOGUE OF TRILOBITES. 
 
 VOGDES.] 
 
 109 
 
 Dalmanites [Dalmania\ aspectans Hall, 1861; Des. New Species Foss., p. 60 (in 
 error D. adspectans). 
 
 [ Dalmania ] aspectans Hall, 1862 ; 15tli Rept. New York State Cab. Nat. Hist., 
 
 p. 88 (in error D. adspectans). 
 
 Syn., Dalmania helena Hall, 1861 ; Des. New Species Foss., p. 61. 
 
 Dalmania helena Hall, 1862 ; 15th Rept. New York State Cab. Nat. Hist., 
 p. 89. 
 
 Dalmanites ohioensis Meek, 1871 ; Proc. Acad. Nat. Sci. Phila., p. 91. 
 Dalmanites ohioensis Meek, 1873 ; Pal. Ohio, vol. 1, p. 234, pi. 23, fig. 1. 
 Dalmanites denticulatus Hall, 1876; Illus. Devonian Foss. Crust., pi. 10, 
 
 fig. 1. 
 
 aspectans Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 13, figs. 6-8. 
 
 Syn., helena Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 13, figs. 13, 14. 
 
 [ Coronura ] aspectans Hall, 1888; Pal. New York, vol. 7, p. 33, pi. 12, figs. 
 
 1-11, 13. 
 
 [ Cryphceus ] barrisi Hall. (See Cryphaeus barrisi Hall.) 
 
 bebryx Billings, 1860; Canadian Naturalist, vol. 5, p. 62, fig. 8. Trenton. 
 
 bebryx Billings, 1863; Geol. Canada, p. 187, fig. 185. 
 
 [Dalmania] bifida Hall, 1861 ; Des. New Species Foss., p. 63. Upper Helderberg. 
 
 [ Dalmania ] bifida Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 
 
 91. 
 
 [ Odontocephalus ] bifida Hall and Clarke, 1888; Pal. New York, vol. 7, p. 53, pi, 
 
 11 b, figs. 22-25. 
 
 Compare Dalmanites cegeria Hall. 
 
 [ Dalmania ] boothi. (See Cryphaeus boothi Green.) 
 
 bicornis Hall, 1875; 28th Rept. New York State Mus. Nat. Hist. Expl., pi. 33, 
 
 fig* 18. Niagara. 
 
 bicornis Hall, 1879; 28th Rept. New York State Mus. Nat. Hist., p. 196, pi. 33, 
 
 fig. 18. 
 
 bicornis Hall, 1882; 11th Aun. Rept. Geol. Nat. Hist. Indiana, 1881, p. 342, pi. 
 
 35, fig. 18. 
 
 breviceps Hall, 1866; 24th Rept. New York State Mus. Nat. Hist., p. 223, pi. 8, 
 
 figs. 15, 16. Hudson. 
 
 breviceps Miller, 1874; Cincinnati Quart. Jour. Sci., vol. 1, p. 143. 
 
 breviceps Hall and Whitfield, 1875 ; Pal. Ohio, vol. 2, p. 108, pi. 4, figs. 15, 
 
 16. 
 
 [ Phacops ] callicephalus Hall, 1847; Pal. New York, vol. 1, p. 247, pi. 65, figs. 
 
 3a-3i. Trenton. 
 
 [Phacops] callicephalus Hall, 1851; Rept. Geol. Lake Superior Land Dist. 
 
 (Foster and Whitney), vol. 2, p. 212, pi. 3, figs. 3 a, 3 b. 
 
 [ Phacops'] callicephalus Emmons, 1855; Am. Geology, vol. 1 , pt. 2, p. 214, pi. 
 
 15, figs. 7, 7 a. 
 
 [ Dalmania] calliteles. (See Cryphaeus calliteles). 
 
 [ Dalmania ] calypso Hall, 1861 ; Des. New Species Foss., p. 61. 
 
 Upper Helderberg. 
 
 [Dalmania] calypso Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., 
 
 p. 89. 
 
 calypso Hall, 1876; Illus. Devonian Foss. Crust., pi. 13, figs. 1,2. 
 
 [Cliasmops] calypso Hall, 1888; Pal. New York, vol. 7, p. 4, pi. 16a, fig. 1. 
 
 ? cayahogoe Claypole, 1884; Geol. Mag., vol. 1, p. 305, figure. Carboniferous. 
 ? cayahogoe Woodward, 1884; Mon. Brit. Carboniferous Tril., p. 79, figure. 
 
 carleyi Meek, 1872; Am. Jour. Sci., 3d series, vol. 3, p. 424. Hudson. 
 
 — — carleyi Meek, 1873; Pal. Ohio, vol. 1, p. 170, pi. 14, iigs. 2a-2d. 
 
 carleyi Miller, 1871 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 142. 
 
 — — [ Dalmania ] eaudata (Brong.) Roomer. (Soo Dalmanites limulurus Green.) 
 
110 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63 . 
 
 Dalmanites [ Crijpliceus ] comis. (See Cryphseus comis Hall.) 
 
 concinnus Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 10, figs. 3-5. Schoharie. 
 
 [ Raxismannia ] concinnus Hall, 1888 ; Pal. New York, vol. 7, p. 30, pi. 11 a, figs. 
 
 9-11. 
 
 [ Hausmannia ] concinnus var. serrula Hall and Clarke, 1888; Pal. New York, 
 
 vol. 7, p. 30, pi. 11 a, fig. 12. 
 
 [ Dalmania ] coronatus Hall, 1861 ; Des. New Species Foss., p. 58. 
 
 Upper Helderberg. 
 
 [Dalmania'] coronatus Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., 
 
 p. 86. 
 
 coronatus Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 12, figs. 15-17 ; pi. 13, 
 
 fig. 5. 
 
 [Odontocephalus ?] coronatus Hall, 1888; Pal. New York, vol. 7, p. 54, pi. 11 b, 
 
 figs. 12-14. 
 
 danae Meek and Worthen, 1865; Pros. Acad. Nat. Sci. Phila., p. 264. Niagara. 
 
 danae Meek and Worthen, 1868 ; Pal. Illinois, vol. 3, p. 363, pi. 6, figs. 1 a-1 f. 
 
 dentata Barrett, 1876 ; Am. Jour. Sci., 3d series, vol. 11, p. 200, plate. 
 
 Lower Helderberg. 
 
 dentata Barrett, 1876; Am. Jour. Sci., 3d series, vol. 12, p. 70. 
 
 [ Corycephalus] dentatus Hall and Clarke, 1888; Pal. New York, vol. 7, p. 58, 
 
 pi. 11 a, figs. 4-6. 
 
 [ Asaphus? ] denticulatus Conrad, 1841; 5th Rept. Pal. Dept. New York Geol. 
 
 Survey, p. 48. 
 
 Lower Helderberg. 
 
 denticulatus Hall, 1876; Illus. Devonian Foss. Crust., pi. 10, fig. 1. 
 
 [ Phceton ] denticulatus Meek, 1877 ; U. S. Geol. Expl. 40th Par., vol. 4, p. 49, 
 
 pi. 1, figs. 10 a, b. 
 
 emarginatus Hall, 1876; Illus. Devonian Foss. Crust., pi. 10, fig. 2. . 
 
 Upper Helderberg. 
 
 [Coronura] emarginatus Hall, 1888; Pal. New York, vol. 7, p. 40, pi. 11 a, figs. 
 
 7, 8. 
 
 epicrates Billings, 1863 ; Proc. Portland Soc. Nat. Hist., vol. 1, p. 119, pi. 1, fig. 21. 
 
 [Dalmania] erina Hall, 1861 ; Des. New Species Foss., p. 62. 
 
 Upper Helderberg. 
 
 [Dalmania] erina Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 90. 
 
 erina Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 13, figs. 3, 4. 
 
 [Chasmops] erina Hall, 1888; Pal. New York, vol. 7, p. 67, pi. 11, figs. 16-18. 
 
 Upper Silurian. 
 
 [Dalmania] helena. (See Dalmanites aspectans.) 
 
 intermedius Walcott, 1877; Advance sheets 31st Rept. New York State Cab. 
 
 Nat. Hist., p. 17. Trenton. 
 
 intermedius Walcott, 1879; 31st Rept. New York State Cab. Nat. Hist., p. 69. 
 
 [Phacopsf] laticauda Hall, 1847 ; Pal. New York, vol. 1, p. 248, pi. 64, fig. 3. 
 
 [Asaphus] limulurus Green, 1832; Monthly Am. Jour. Geol., vol. 1, p. 559. 
 
 Niagara. 
 
 [Asaphus] limulurus Green, 1832; Mon. Tril. N. A., p. 48, cast 16. 
 
 [Phacops] limulurus Hall, 1852; Pal. New York, vol. 2, p. 303, pi. 67, figs. 1-8. 
 
 Syn. [Dalmania] caudata (Brong.) Roemer, 1860; Die sil. Fauna W. Tenn..p. 82, 
 pi. 5, fig. 21. 
 
 [Dalmania] logani Hall, 1860; Canadian Naturalist, vol. 5, p. 156, fig. 18. ' 
 
 Silurian. 
 
 [Dalmania] macrops Hall, 1861 ; Des. New Species Foss., p. 59. 
 
 Upper Helderberg. 
 
 [Dalmania] macrops Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., 
 
 p. 87. 
 
VOGDKS.] 
 
 CATALOGUE OF TR1LOB1TES. 
 
 Ill 
 
 Dalmanites macrops, 1876 ; Illus. Devonian Foss. Crust., pi. 13, figs. 9, 10. 
 
 [ Chasmops ] macrops Hall, 1888; Pal. New York, vol. 7, p. 68, pi. 11 a, figs. 
 
 14, 15. 
 
 macroura ? (Sjogr.) Billings, 1866; Catalogue Sil. Foss. Anticosti, p. 61. 
 
 [ Dal mania ] meta Hall, 1862; Geol. Wisconsin, vol. 1, p. 433. 
 
 meeki Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 207, 
 
 pi. 17, figs. 5-5 a, b (not fig. 5 c). 
 
 (undetermined sp.) Meek, 1877 ; U. S. Geol. Expl. 40th Par., vol. 4, p. 48, pi. 1, 
 
 figs. 11, 11 a. 
 
 [ Hausmannia ] meeki Hall, 1888 ; Pal. New York, vol. 7, p. 11 a, figs. 28-30. 
 
 lAsaphus] micrurus Green, 1832; Monthly Am. Jour. Geology, p. 559, pi. 14, 
 
 fig. 3. Lower Helderberg. 
 
 [ Asaphus ] micrurus Green, 1832 ; Mon. Tril. N. A., p. 56, cast 19, pi., fig. 3. 
 
 .{Dalmania ] micrurus Hall, 1859 ; Pal. New York, vol. 3, p. 359, pi. 75, figs. 13-18. 
 
 \_AsapTius'] myrmecophorus Green, 1835; Am. Jour. Sci., 1st series, vol. 23, p. 
 
 397. Upper Helderberg. 
 
 [Asaphus ] myrmecophorus Green, 1835; Suppl. Mon. Tril. N. A.,p. 16, cast 40. 
 
 [J Dalmania] myrmecophorus Hall, 1861; Des. New Species Foss., p. 60. 
 
 [ Dalmania ] myrmecophorus Hall, 1862 ; 15th Kept. New York State Cab. Nat. 
 
 Hist., p. 88. 
 
 myrmecophorus Hall, 1876; Illus. Devonian Foss. Crust., pi. 13, figs. 15, 16. 
 
 [Coronura] myrmecophorus Hall, 1888 ; Pal. New York, vol. 7, p. 37, pi. 11 a, 
 
 fig. 13 ; pi. 13, fig. 12; pi. 14, figs. 1-6 ; pi. 15, figs. 1-4. 
 
 [Asaphus] nasutus Conrad, 1841 ; 5th Kept. Pal. Dept. New York Geol. Survey, 
 
 p. 48. Lower Helderberg. 
 
 [ Dalmania ] nasutus Hall, 1859 ; Pal. New York, vol. 3, p. 362, pi. 75, fig. 2 ; 
 
 pi. 76, figs. 1-9. 
 
 [ Dalmanites'] ohioensis. (See Dalmanites aspectans.) 
 
 [ Hausmannia ] phacoptyx Hall, 1888; Pal. New York, vol. 7, p. 31, pi. 11 a, 
 
 figs. 23-29. Upper Helderberg. 
 
 [Dalmania] pleione. (See Cryphaeus pleione.) 
 
 [Asaphus] pleuropteryx Green, 1832; Monthly Jour. Geol., vol. 1, p. 559. 
 
 Lower Helderberg. 
 
 [ Asaplius ] pleuropteryx Green, 1832; Mon. Tril. N. A., p. 55, cast 18. 
 
 [ Dalviania ] pleuropteryx Hall, 1859; Pal. New York, vol. 3, p. 356, pi. 74, figs. 
 
 5 (?) 9 (?) (not figs. 1-4, 6-8, 10-12), pi. 75, fig. 1. 
 
 [Hausmannia] pleuropteryx Hall, 1888; Pal. New York, vol. 7, p. 28, pi. 9, 
 
 > figs. 1-3. 
 
 — — [ Corycephalus ] pygmaeus Hall, 1888; Pal. Now York, vol. 7, p. 56, pi. 11, figs. 
 5-8. Upper Helderberg. 
 
 regalis Hall, 1876; Illus. Devonian Foss. Crust., pi. 11, figs. 1-4. 
 
 Upper Helderberg. 
 
 - — [Corycephalus] regalis Hall, 1888; Pal New York, vol. 7, p. 55, pi. 11, figs. 1-4. 
 
 [ Asaplius ] selenurus Eaton, 1832; Geological Text Book, pi 31, pi. 1, fig. 1. 
 
 Upper Helderberg. 
 
 [Asaphus] selenurus Green, 1832 ; Mon. Tril. N. A., p. 46, casts 14 and 15. 
 
 Syn., Calymene? odontocephala Green, 1835; Suppl. Mon. Tril. N. A., p. 9, cast 36. 
 Calymenef odontocephala Green, 1835; Am. Jour. Sci., 1st series, vol. 25, p. 
 334. 
 
 [Odontocephalus] selenurus Conrad, 1840; 3d Rept. Pal. Dept. New York Geol. 
 
 Survey, p. 204. 
 
 [Odontocephalus] selenurus Vanuxom, 1842; Geol. New York, 3d Geol. Dist., 
 
 pp. 139, 140, fig. 1. 
 
 [Odontocephalus] selenurus Hall, 1843; Geol. Now York, 4th Geol. Dist., p. 175, 
 
 fig. 1. 
 
112 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63. 
 
 Dalmanites [ Dalmania ] selenurus Hall, 1859 ; 12th Rept. New York State Cab. 
 Nat. Hist., p. 88. 
 
 [ Dalmania ] selenurus Hall, 1861; Des. New Species Foss.,p. 56. 
 
 [ Dalmania ] selenurus Hall, 1862 ; 15th Rept. New York State Cab. Nat. Hist., 
 
 p. 84. 
 
 Syn., Odontocephalus? ( Dalmanites-Odontocephalus ) arenarius Meek and Worthen, 
 1868; Geol. Survey Illinois, vol. 3, p. 416, pi. 9, fig. 10. 
 
 selenurus Hall, 1876; Illus. Devonian Foss. Crust., pi. 12, figs. 12-14. 
 
 [Odontocephalus ] selenurus Hall, 1888; Pal. New York, vol. 7, p. 49, pi. 11 b, figs. 
 
 15-21 ; pi. 12, figs. 1-13. 
 
 [Dalmania] tridens Hall, 1859; Pal. New York, vol. 3, p. 361, pi. 75, figs. 3-6. 
 
 Lower Helderberg. 
 
 [ Dalmania ] tridentifera Shumard, 1855; 1st and 2d Geol. Repts. Missouri, 
 
 p. 199, pi. B, figs. 8 a-c. Lower Helderberg. 
 
 tridentifera Meek and Worthen, 1868; Pal. Illinois, vol. 3, p. 391, pi. 7, fig. 16. 
 
 troosti Safford, 1869; Geol. Tennessee, p. 290. (See Chasmops troosti Safford.) 
 
 Nashville. 
 
 [Dalmania] verrucosus Hall, 1863; Trans. Albany Inst., vol. 4, p. 218. (Ab- 
 stract published May, 1863, p. 24.) Niagara. 
 
 verrucosus Hall, 1875; 28th Rept. New York State Mus. Nat. Hist., pi. 23, figs. 
 
 5-17, 13-15. Museum ed., 1879, p. 195, pi. 23, fig. 5-17; pi. 34, figs. 13-15. 
 
 verrucosus Hall, 1882; 11th Ann. Rept. Dept. Geol. Nat. Hist. Indiana, p. 341, 
 
 pi. 35, figs. 5-17; pi. 36, figs. 13-15. 
 
 vigilans Hall, 1861 ; Rept. Progress Wisconsin Geol. Survey, p. 51. Niagara. 
 
 [ Dalmania 3 . vigilans Hall, 1867 ; 20th Rept. New York State Cab. Nat. Hist., 
 
 p. 335, pi. 21, figs. 16-18. 
 
 [Dalmania] vigilans Hall, 1870; 20th Rept. New York State Cab. Nat. Hist. (2d 
 
 ed.), p. 426, pi. 21, figs. 16-18. 
 
 vigilans Hall, 1875; 28th Rept. New York State Mus. Nat. Hist. Expl., pi. 33, 
 
 figs. 1-4. 
 
 vigilans Hall, 1879; 28th Rept. New York State Mus. Nat. Hist. (Mus. ed.), p. 
 
 193, pi. 33, figs. 1-4. 
 
 vigilans Hall, 1882 ; 11th Ann. Rept. Geol. Nat. Hist. Indiana, 1881, p. 339, pi. 35, 
 
 figs. 1-4 ; pi. 33, fig. 9. 
 
 werthneri Foerste, 1885 ; Bull. Denison Univ., vol. 1, p. 116. Clinton. 
 
 werthneri Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 109, pi. 8, figs. 22-25. 
 
 Dicellocephalus. (See Dikelocephalus.) 
 
 Dikelocephalus Owen, 1852 ; Rept. Geol. Survey Wisconsin, Iowa, and Minnesota, 
 p. 573. 
 
 Type, Dikelocephalus minnesotensis Owen. 
 
 Syn., Centropleura Angelin, 1854 ; Pal. Scand., p. 87, pi. 41, figs. 9-11. 
 
 This generic term has sometimes been spelled Dicellocephalus. 
 
 affinis Billings, 1865 ; Pal. Foss., vol. 1, p. 197, fig. 183 a,, b. Quebec, 
 
 ? angustifrons Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8. 
 
 p. 42, pi. 10, figs. 1,1 a, b. Cambrian. 
 
 belli Billings, 1860 ; Canadian Naturalist, vol. 5, p. 311, fig. 7. Quebec. 
 
 belli Billings, 1865 ; Pal. Foss., vol. 1, p. 403, fig. 378. 
 
 barabuensis Whitfield, 1878; Ann. Rept. Geol. Survey Wisconsin, 1877, p. 63. 
 
 Uower Magnesian. 
 
 barabuensis Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 201, pi. 4, figs. 6-9. ■ 
 
 Compare Bathyurus capax Billiugs. 
 
 bilobatus Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par., p. 226, pi. 2, 
 
 fig. 36. Potsdam. 
 
 bilobatus Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 40. 
 
V0GDE3.] 
 
 CATALOGUE OF TRILOB1TES. 
 
 113 
 
 Dikelocephalus crassimarginatus Whitfield, 1882 ; Geol. Wisconsin, vol. 4, p. 344, 
 pi. 27, fig. 14. ' Potsdam. 
 
 Syn pepinensis (Hall), 16th Kept. New York State Cab. Nat. Hist. Expl., pi. 11. 
 fig. 2. • 
 
 ? corax Billings, 1865; Pal. Foss., vol. 1, p. 344, figs. 322 a, b. Quebec. 
 
 Referred to Olenoides f corax Walcott, 1884; Bull. U. S. Geol. Survey, No. 30, 
 p. 184. 
 
 cristatus Billings, 1860 ; Canadian Naturalist, vol. 5, p. 312, fig. 10. Quebec. 
 
 cristatus Billings, 1865 ; Pal. Foss., vol. 1, p. 404, fig. 384. 
 
 This species might be referred to the genus Dorypyge. 
 
 devinei Billings, 1865; Pal. Foss., vol. 1, p. 195, figs. 180,181. Quebec. 
 
 eatoni Whitfield, 1878 ; Ann. Rept. Geol. Survey Wisconsin, 1877, p. 65. 
 
 Lower Magnesian. 
 
 eatoni Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 202, pi. 4, figs. 11-17; pi. 10, 
 
 figs. 4, 5. 
 
 ? expansus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 89, pi. 9, fig. 19. Cambrian. 
 
 finalis Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 89, 
 
 pi. 12, figs. 12 a,b. Pogonip. 
 
 flabellifer Hall and Whitfield, 1877; U. S. Geol. Expl. 40th Par., vol. 4, p. 227, 
 
 pi. 2, figs. 29, 30. Potsdam. 
 
 flagricaudus White. (See Olenoides? flagricauda.) 
 
 ? gothicus Hall and Whitfield. (See Dorypyge gothicus.) 
 
 hisingeri Billings, 1865; Pal. Foss., vol. 1, p. 196, fig. 182. Quebec. 
 
 inexpectans Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 90, pi. 1, fig. 10. Pogonip. 
 
 ? iowensis Owen. (See Crepicephalus iowensis (Owen) Walcott.) 
 
 iole Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 43, 
 
 pi. 10, fig. 19. Cambrian. 
 
 latifrons Shumard, 1863; Trans. Acad. Sci. St. Louis, vol. 2, p. 101. Potsdam. 
 
 lodensis Whitfield, 1880; Ann. Rept. Geol. Survey Wisconsin, 1879, p. 51. 
 
 Potsdam. 
 
 lodensis Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 188, pi. 10, fig. 14 ; p. 341, 
 
 pi. 27, figs. 12, 13. 
 
 magnificus Billings, i860 ; Canadian Naturalist, vol. 5, p. 307, fig. 5 ( Bemoplcn - 
 
 rides magnificus Billings, 1865; Pal. Foss., vol. 1, p. 294). Quebec. 
 
 magnificus Billings, 1865 ; Pal. Foss., vol. 1, p. 399, fig. 376. 
 
 ? marcoui Whitfield, 1884 ; Bull. Am. Mus. Nat. Hist. New York, vol. 1, p. 150, 
 
 pi. 14, fig. 7. Potsdam. 
 
 Referred to Olenoides marcoui Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, 
 p. 186, pi. 26, figs. 5, 5 a, b. 
 
 marica Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 44, 
 
 pi. 10, fig. 13. Cambrian. 
 
 megalop Billings, 1860 ; Canadian Naturalist, vol. 5, p. 311, fig. 9. Quebec. 
 
 megalop Billings, 1865; Pal. Foss., vol. 1, p. 403, fig. 380. 
 
 mini8caensi8. (See Ptychaspis miniscaensis.) 
 
 minnesotensis Owen. Cambrian. 
 
 A very large sp. Asaphus Owen, 1848; Rept. Geol. Reconnoissance Chippewa 
 Land Dis., p. 15, pi. 7, figs. 2, 3. 
 
 minnesotensis Owen, 1852; Rept. Geol. Survey Wisconsin, Iowa, and Minne- 
 sota, p. 574, pi. 1, figs. 2, 10; pi. 10, figs. 3, 6. 
 
 minnesotensis Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 138, 
 
 pi. 9, figs. 5-10 ; pi. 10, figs. 10-12 ; pi. 11, figs. 1-4, 6. 
 
 Bull. 63 8 
 
114 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63 . 
 
 Bikeiocephalus minnesotensis var. limbatus Hall, 1863; 16th Rept. New York 
 State Cab. Nat. Hist., p. 141, pi. 9, fig. 12. 
 
 ; minnesotensis var. Hall. 1863; 16th Rept. New York State Cab. Nat. Hist., p. 
 
 141, pi. 9, fig. 11; pi. 10, fig. 9. 
 
 minnesotensis Winchell, 1864 ; Am. Jour. Sci., 2d series, vol. 37, p. 229. 
 
 minnesotensis Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 187, pi. 3, fig. 1. 
 
 misa Hall, 1863; 16th Rept. State Cab. Nat. Hist., p. 144, pi. 8, fig. 15 ; pi. 10, 
 
 figs. 4-8. Potsdam. 
 
 missisquoi Billings, 1865; Pal. Foss., vol. 1, p. 199. Quebec. 
 
 multicinctus Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par., vol. 4, p. 
 
 226, pi. 2, fig. 37. Potsdam. 
 
 nasutus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 40, 
 
 pi. 10, fig. 15. Cambrian. 
 
 osceola Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 146, pi. 7, 
 
 fig. 49 ; pi. 10, fig. 18. Potsdam. 
 
 osceola Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8,p. 40, 
 
 pi. 9, fig. 25. 
 
 oweni Billings, 1860; Canadian Naturalist, vol. 5, p. 310, fig. 8. Quebec. 
 
 oweni Billings, 1865; Pal. Foss., vol. 1, p. 402, fig. 379. 
 
 pauper Billings, 1865; Pal. Foss., vol. 1, p. 200. Quebec. 
 
 pepinensis Owen, 1852 ; Rept. Geol. Survey Wisconsin, Iowa, and Minnesota, 
 
 p. 574, pi. 1, figs. 9, 9 a; pi. 1 a, fig. 7. Potsdam. 
 
 pepinensis Hall, 1863 ; 16th Rept. New York State Cab. Nat. Hist., p. 142, pi. 9, 
 
 figs. 1-4 ; pi. 10, figs. 13-17. (Expl., pi. 11, fig. 2. See Dicellocephalus 
 crassimarginatus. ) 
 
 pepinensitf'Winchell, 1864 ; Am. Jour. Sci., 2d series, vol. 37, p. 229. 
 
 planifrons Billings, 1860; Canadian Naturalist, vol. 5, p. 309, fig. 6. Quebec. 
 
 planifrons Billings, 1865; Pal. Foss., vol. 1, p. 401, fig. 377. 
 
 quadriceps. (See Dorypyge quadriceps.) 
 
 richmondensis Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 
 
 8, p. 41, pi. 10, fig. 7. Cambrian. 
 
 roemeri Shumard, 1861 ; Am. Jour. Sci., 2d series, vol. 32, p. 220. Potsdam. 
 
 selectus Billings, 1865; Pal. Foss., vol. 1, p. 199. Quebec. 
 
 selectus Billiugs, 1865; Pal. Foss., vol. 1, p. 198. (See Ptychaspis selectus.) 
 
 spiniger Hall, 1863; 16ih Rept. New York State Cab. Nat. Hist., p. 143, pi. 10, 
 
 figs. 1, 2, 3(?). Potsdam. 
 
 wahsatchensis. (See Olenoides wahsatchensis.) 
 
 Dionide Barrande, 1847 ; Neues Jahrbuch fur Mineral., vol. 4, p, 391. 
 
 Type, Dionide formosa Barrande. 
 
 Syn., Dione Barrande; Notice Prelim. Sil. Syst. Boheme, p. 33. 
 
 Polytomurus Corda, 1847 ; Prodr., p. 153. 
 
 ? perplexa Billings, 1866 ; Catalogue Sil. Foss. Anticosti, p. 67. 
 
 Dipleura Green, 1832; Mon. Tril. North America, p. 79. (See Homalonotus de- 
 kayi.) 
 
 Discranurus Conrad, 1841 ; 5th Rept. Pal. Dept. New York Geol. Survey, p. 48. (See 
 Acidaspis liamata.) 
 
 Dolichometopus Angelin, 1854 ; Palseont. Scand., p. 72. 
 
 Type, Dolichometopus sveticus Ang. 
 
 ? convexus Billings, 1865; Pal. Foss., vol. 1, p. 269, fig. 253. 
 
 ? gibberrulus Billings, 1865 ; Pal. Foss., vol. 1, p. 269, fig. 254. 
 
 ? rarus Billings, 1865 ; Pal. Foss., vol. 1, p. 352, fig. 308. 
 
 Dorypyge Dames, 1684; China (Richthofen), vol. 4, p. 23. 
 
 Type, Dorypyge richthofeui Dames. 
 
 [ Dihelocephalus ] cristatus Billings, 1865 ; Pal. Foss., vol. 1, p. 404, fig. 384. 
 
 Cambrian, 
 
 Quebec. 
 
 Quebec. 
 
 Quebec. 
 
VOGDES. j 
 
 LIST OF TRILOBITES. 
 
 115 
 
 Dorypyge IDikeloccphalus f] gothicus Hall and Whitfield, 1877 ; U. S. Geol. Expl. 
 
 40th Par., vol. 4, p. 242, pi. 1, fig. 36. Potsdam. 
 
 gothicus Dames, 18^4; China (Richthofen), vol. 4,p. 23. 
 
 [Dicellocephalus ?] gothicus Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. 
 
 Survey, vol. 8, p. 45, pi. 9, fig. 24. Referred to 
 
 [Olenoides ] gothicus Walcott, 1886; Bull. U. S. Geol. Survey, vol. 30, p. 187, pi. 
 
 29, figs. 1, 1 a-c. 
 
 [ Dikelocephalus ] quadriceps Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th 
 
 Par., vol. 4, p. 240, pi. 1, tigs. 37-40. Cambriau. 
 
 [ Dicellocephalus ] quadriceps Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. 
 
 Survey, vol. 8, p. 45, pi. 9, fig. 24. 
 
 quadriceps Dames, 1884; China (Richthofen), vol. 4,p. 23. Referred to 
 
 [ Olenoides~\ quadriceps Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 187, pi. 
 
 29, figs. 1, 1 a-c. 
 
 Dysplanus Burmeister, 1843; Organization of Trilobites (Ray Soc. ed.,p. 205). 
 
 Type, Dysplanus centrotus Dalman. 
 
 Ellipsocephalus Zenker, 1833; Beitriige Naturgeschichte der Urwelt, p. 51. 
 
 Type, Ellipsocephalus hoffi Bronn. 
 
 curtus Whitfield, 1878; Ann. Rept. Geol. Wisconsin, 1877, p. 58. Potsdam. 
 
 cjirtus Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 191, pi. 1, fig. 18. 
 
 Eliptocephalus Emmons, 1844; Taconic Syst., p. 21, figs. 1-3. 
 
 asaphoides. (See Olenellus asaphoides Emmons.) 
 
 Embolimus Rominger, 1887 ; Proc. Acad. Nat. Sci. Phila., p. 16. (See Zacanthoides 
 Walcott.) 
 
 rotundata. (See Bathyuriscus howelli.) 
 
 spinosa. (See Olenoides spinosus.) 
 
 Encrinurus Emmricli, 1844; Zur Naturg. Trilobiten, p. 16. 
 
 Type, Encrinurus punctatus Briinnich. 
 
 americanus Vogde.s, 1886; Des. New Crust. Clinton Group Georgia, p. 1. 
 
 Clinton. 
 
 americanus Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 102. 
 
 deltoideus Shumard, 1855; Geol. Missouri, p. 198, pi. B, fig. 10. 
 
 Upper Silurian- 
 
 [ Cryplonymus ] deltoideus Yogdes, 1878; Mon. Genera Zethus, etc., p. 21. 
 
 deltoideus Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 102. 
 
 egani Miller, 1879; Jour. Cincinnati .Soc. Nat. Hist., vol. 2, p. 254, pi. 15, figs. 
 
 1, l a, b. Niagara. 
 
 elegantulus Billings, 1866 ; Catalogue Sil. Foss. Anticosti, p. 62. 
 
 elegantulus Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 102. 
 
 excedrensis Saflord. (See Encrinurus varicostatus Walcott.) 
 
 Syn., excedrensis Safford, 1869; Geol. Tennessee, p. 290. 
 
 mirus Billings, 1865; Pal. Foss., vol. 1, p. 292, fig. 282. Quebec. 
 
 [ Cryptonymus~\ mirus Yogdes, 1878 ; Mon. Genera Zethus, etc., p. 34. 
 
 [Amphion] multisegmentatus Portlock, 1843; Geol. Londonderry, etc., p. 291, 
 
 pi. 3, fig. 6. 
 
 multisegmentatus Salter ; Mem. Geol. Survey United Kingdom, decade 7, pi. 4. 
 
 multisegmentatus Billings, 1866; Catalogue Sil. Foss. Anticosti, p. 61. 
 
 [Cryptonymus] multisegmentatus Vogdes, 1878 ; Mon. Genera Zethus, etc., p. 29. 
 
 nereus Hall, 1867 ; 20tli Rept. Now York State Cab. Nat. Hist., p. 375, pi. 21, 
 
 fig. 15. Niagara. 
 
 nereus Hall, 1870 ; 20th Rept. New York State Cab. Nat. Hist., p. 425, pi. 21, 
 
 fig. 15. 
 
 [ Cryptonymus ] nereus Vogdes, 1878 ; Mon. Genera Zethus, etc., p. 24, pi. 3, fig. 17. 
 
 ornatus Hall and Whitfield, 1875; Pal. Ohio, vol. 2, p. 154, pi. 7, fig. 16. 
 
 Niagara. 
 
 Syn., Cybele punctata Hall, 1852 ; Pal. New York, vol. 2, p. 297, pi. A 66, figs, 1 a-k. 
 
116 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63 . 
 
 Encrinurus [ Cryptonymus ] ornatus Yogdes, 1878; Mon. Genera Zethus, etc., p. 23. 
 
 ornatus Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 102. 
 
 punctatus (Briinnich) Billings, 1866; Catalogue Sil.'Foss. Anticosti, p. 61. 
 
 thresheri Foerstfc, 1887 ; Bull. Denison Univ., vol. 2, p. 101, pi. 8, fig. 26. 
 
 Clinton. 
 
 trentonensis Walcott, 1877; Advance sheets 31st Rept. New York State Mus. 
 
 Nat. Hist., p. 15. Trenton. 
 
 trentonensis Walcott, 1879; 31st Rept. New York State Mus. Nat. Hist., p. 
 
 68 . 
 
 [ Cryptonymus ] trentonensis Yogdes, 1878; Mon. Genera Zethus, etc., p. 28. 
 
 varicostatus Walcott, 1877 ; Advance sheets 31st Rept. New York State Mus^ 
 
 Nat. Hist., p. 16. Trenton. 
 
 varicostatus Walcott, 1879 ; 31st Rept. New York State Cab. Nat. Hist., p. 69. 
 
 [Cryptonymus J varicostatus Yogdes, 1878; Mon. Genera Zethus, etc., p. 27. 
 
 varicostatus Safford and Yogdes, 1889 ; Proc. Acad. Nat. Sci. Phila., p. 167, 
 
 figure. 
 
 [ Ceraurus ] vigilans Hall, 1847 ; Pal. New York, vol. 1, p. 245, pi. 65, figs. 2a-2 h. 
 
 Trenton. 
 
 [ Ceraurus ] vigilans Emmons, 1855; Am. Geology, vol. 1, pt. 2, p. 217, pi. 15, 
 
 figs. 2 a-2 c. 
 
 [ Cryptonymus ] vigilans Vogdes, 1878; Mon. Genera Zethus, etc., p. 29, pi. 2, 
 
 figs. 2 a-2 h. 
 
 Endymion Billings, 1862; Pal. Foss., vol. 1, p. 94. Changed by author to Endy- 
 mionia. 
 
 Endymionia Billings, 1865; Pal. Foss., vol. 1, p. 281. 
 
 meeki Billings, 1862 ; Pal. Foss., vol. 1, pp. 94 and 281, fig. 84. Quebec. 
 
 Griffithides Portlock, 1843; Geol. Rept. Londonderry, etc., p. 310. 
 
 Type, Griffithides longiceps Portlock.' 
 
 [ Phillipsia ( Griffithides )] bufo Meek and Worthen, 1870; Proc. Acad. Nat. Sci. 
 
 Phila., p. 52. Keokuk. 
 
 [Phillipsia (Griffithides)] bufo Meek and Worthen, 1873; Geol. Survey Illinois, 
 
 vol. 5, p. 528, pi. 19, fig. 5. 
 
 bufo Yogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 95, pi. 3, figs. 4, 5, 10. 
 
 [ Proetus] granulatus Wetherby, 1881 ; Jour. Cincinnati Soc. Nat. Hist., vol. 4, 
 
 p. 31, pi. 2, figs. 8, 8 a, 9, 9 a. Chester. 
 
 granulatus Yogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 101. 
 
 [ Phillipsia (Griffithides lodiensis Meek. (See Brachymetopsis lodiensis.) 
 
 [ Phillipsia ( Griffithides )] portlocki Meek and Worthen, 1865; Proc. Acad. Nat. 
 
 Sci. Phila., p. 268. Keokuk. 
 
 [ Phillipsia (Griffithides)'] portlocki Meek and Worthen, 1873 ; Geol. Survey Illi- 
 nois, vol. 5, p. 525, pi. 19, fig. 6. 
 
 portlocki Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 266, pi. 24, figs. 4, 4 a, b. 
 
 portlocki Yogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 93, pi. 3, fig. 9. 
 
 [. Phillipsia ( Griffithides ?)] sangamonensis Meek and Worthen, 1865; Proc. 
 
 Acad. Nat. Sci. Phila., p. 270. Coal Measures. 
 
 [ Phillipsia (Griffithides ?)] sangamonensis Meek and Worthen, 1873; Geol. Sur- 
 vey Illinois, vol. 5, p. 615, pi. 32, fig. 4. 
 
 [ Phillipsia (Griffithides ?)] sangamonensis White, 1883; 13th Rept. Dept. Geol. 
 
 Nat. Hist. Indiana, p. 174, pi. 39, figs. 4,5. . 
 
 [ Phillipsia ] sangamonensis Herrick, 1887 ; Bull. Denison Univ., vol. 2, p. 61, 
 
 pi. 5, fig. 13. 
 
 [ Griffithides ] sangamonensis Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, 
 
 p. 99, pi. 3, figs. 7, 8. 
 
 [ Phillipsia (Griffithides)] scitula Meek and Worthen, 1865; Proc. Acad. Nat. Sci. 
 
 Phila. , p. 270. Coal Measures. 
 
vogdes.] CATALOGUE OF TRILOBITES. 117 
 
 Griffithides [ Phillipsia ( Griffithides )] scitula Meek and Wortlien, 1873; Geol. Survey 
 Illinois, vol. 5, p. 612, pi. 32, fig. 3. 
 
 [ Phillipsia ( Griffithides )] scitula While, 1883; 13th Ann. Kept. Dept. Geol. Nat. 
 
 Hist. Indiana, 1882, p. 173, pi. 39, figs. 6-9. 
 
 iPhillipsia] scitula Meek, 1872; U. S. Geol. Survey Territories, Final Kept. Ne- 
 braska, p. 238, pi. 6, fig. 9. 
 
 [ Phillipsia ] scitula Herrick, 1887 ; Bull. Denison Univ., vol. 2, p. 62. 
 
 scitula Vogdes, 1887; Annals New York Acarl. Sci., vol. 4, p. 97, pi. 2, figs. 
 
 11-13. 
 
 ? sedaliensis Vogdes, 1888; Trans. New York Acad. Sci., vol. 7, p. 249. 
 
 . Waverlv. 
 
 [Phcethonides ?] sedaliensis Herrick, 1839 ; Bull. Denison Univ., vol. 3, p. 57. 
 
 Harpes Goldfuss, 1839 ; Nova Acta Acad. Loop. Carol., vol. 19, p. 358. 
 
 Type, H'arpes ungula Sternb. 
 
 antiquatus Billings, 1859 ; Canadian Naturalist, vol. 4, p. 469, fig. 38. Ckazy. 
 
 antiquatus Billings, 1863 ; Geol. Canada, p. 133, fig. 67. 
 
 consuetus Billings, 1866; Catalogue Sil. Foss. Anticosti, p. 64. 
 
 dentoni Billings, 1863; Canadian Naturalist, vol. 8, p. 3(5, figure. Trenton. 
 
 c^ntoni Billings, 1865 ; Pal. Foss., vol. 1, p. 183, fig. 166. 
 
 ecanabise Hall, 1851 ; Rept. Geol. Lake Superior Land Dist. (Foster and Whit- 
 ney), pt. 2, p. 211, pi. 27, fig. 2 a. Trenton. 
 
 granti Billings, 1865 ; Pal. Foss., vol. 1, p. 326, fig. 314. 
 
 ottawensis Billings, 1865 ; Pal. Foss., vol. 1, p. 182, fig. 165. Trenton. 
 
 Harpides Beyrich, 1846 ; Untersueh. Trilohiten, p. 34. 
 
 atlanticus Billings, 1865 ; Pal. Foss., vol. 1, p. 281, fig. 267. Quebec. 
 
 concentricus Billings, 1865 ; Pal. Foss., vol. 1, p. 282, fig. 268. Quebec. 
 
 ? desertus Billings, 1865 ; Pal. Foss., vol. 1, p. 333, fig. 321. Quebec. 
 
 Hausmannia Hall, 1888; Pal. New York, vol. 7, p. xxxi. (Subgenus, see Dalma- 
 nites.) 
 
 Hemicr upturns Green, 1832; Mon. Tril. N. A., p. 20. 
 
 clintoni. (See Calymene clintoni Vanuxem.) 
 
 Holometopus Angelin, 1854 ; Pakeont. Scand., p. 58. 
 
 Type, Holometopus aciculatus, pi. 33, fig. 5. 
 
 angelini Billings, 1862; Pal. Foss., vol. l,p. 95, fig. 85; alsop. 281. Quebec. 
 
 Homalonotus Koenig, 1820; leones Foss. Sectiles, p. 4. 
 
 Type, Homalonotus lenighti Koenig, pi. 7, fig. 85. 
 
 Syn., Brongniartia Eaton, 1832; Geological Text Book, p. 32, pi. 2, fig. 20 (in 
 part). 
 
 Dipleura Green, 1832; Mon. Tril. N. A., p. 78; Monthly Am. Jour. Geology, 
 p. 560. 
 
 Trimerus Green, 1832; Mon. Tril. N. A., p. 81 ; Monthly Am. Jour. Geology^ 
 p. 560. 
 
 Plcesiacomia Cord a, 1847; Prodr., p. 171. 
 
 Brogniartia Salter, 1865 ; Mon. Brit. Tril., p. 104 (subgenus). 
 
 Burmei8ieria Salter, 1865; Mon. Brit. Tril., p. 105 (subgenus). 
 
 Koenigia Salter, 1865; Mon. Brit. Tril., p. 104 (subgenus). 
 
 [ Asaphus ] cornigerus (Scblotlieim) Brong., 1822; Crust. Foss., p. 18, pi. 4, fig. 10 
 
 (not pi. 2, fig. 1). 
 
 [ Asaphus ] crypturus Green, 1834; Trans. Geol. So'c. Pennsylvania, vol. 1, p. 37, 
 
 pi. 4. Devonian. 
 
 [ Asaphus ?] crypturus Green, 1835 ; Suppl. Mon. Tril. N. A., p. 18, cast 41. 
 
 Syn., Asaphus ditmarsice Honoyinan, 1879 ; Proc. Nova Scotia Inst., vol. 5, p. 18. 
 
 [ A8aphu8?~\ crypturus Honeyman, 1888; Proc. Nova Scotia lust., vol. 7, pt. 1, 
 
 p. 63. 
 
 dawsoni Hall, 1860; Canadian Naturalist, vol. 5, p. 155. 
 
 Silurian. 
 
118 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Homalonotus dawsoni Dawson, 1878; Acadian Geology (3d ed.), p. 606, fig. 214. 
 
 [ Dipleura ] dekayi Green, 1832 ; Mon. Tril. N. A., p. 79, casts 30, 31, pi. 1, figs. 8, 9. 
 
 Hamilton. 
 
 Syn., Nuttainia sparsa Eaton, 1832; Geological Text Book, p. 34. 
 
 Nuttainia sparsa Green, 1832; Mon. Tril. N. A., p. 89, cast 35. 
 
 I Dipleura'] dekayi Yanuxem, 1842; Geol. New York, 3d Geol. Dist., p. 150, 
 
 fig. 1. 
 
 [Dipleura] dekayi Hall, 1843; Geol. New York, 4th Geol. Dist.,p. 205, fig. 1 
 
 dekayi Emmons, 1860 ; Manual Geology, pp. 146, 147, figs. 134, 135. 
 
 dekayi Hall, 1861 ; Des. New Species Foss, p. 85. 
 
 dekayi Hall, 1862; 15th Rept. New York State Cab. Nat. Hist.,p. 113. 
 
 dekayi Hall, 1877 ; Illus. Devonian Foss. Crust., pis. 2-5. 
 
 dekayi Hall, 1888 ; Pal. New York, vol. 7, p. 7, pi. 2, figs. 1-12 ; pi. 3, figs. 1-5; 
 
 pi. 4, figs. 1-7 ; pi. 5, figs. 1-4. 
 
 [Trimerus] delphinocephalus Green, 1832; Monthly Am. Jour. Geol., vol. 1, p. 
 
 559, pi. 0, fig. 1. Niagara. 
 
 [Trimerus] delphinocephalus Green, 1832; Mon. Tril. N. A., p. 82, pi. 1, fig. 1, 
 
 .cast 32. 
 
 [Trimerus] delphinocephalus Harlan, 1835; Trans. Geol. Soc. Pennsylvania, 
 
 vol. l,p. 105. 
 
 Syn., Brongniartia platycephala Eaton, 1832; Geol. Text Book, p. 32, pi. 2, fig. 20. 
 Brongniartia platycepliala Green, 1832; Mon. Tril. N. A.,p. 91. 
 
 Ogygies latisima Eaton, 183i ; Am. Jour. Sci., 1st series, vol. 21, p. 136 (foot- 
 note). 
 
 delphinocephalus Murchison, 1839 ; Sil. Syst., p. 651, pi. 7 Zns, figs. 1 a, 1 b. 
 
 Syn., Ahrendii Roemer, 1843 ; Yerst. Harzzebirges, p. 39, pi. 11, fig. 5. 
 
 delphinocephalus Hall, 1843 ; Geol. New York, 4th Geol. Dist., p. 103, fig. 34. 
 
 delphinocephalus Yerneuil, Note sur la parall61isme, etc., p. 47. 
 
 Syn., atlas Castelnau, 1843; Syst. Sil. de PAm6r.,p. 20. 
 giganteus Castelnau, 1843 ; Syst. Sil. de FAm6r. 
 herculaneus Castelnau, 1843; idem. 
 
 delphinocephalus Hall, 1852 ; Pal. New York, vol. 2, p. 309, pi. 68, figs. 1-14. 
 
 — — delphinocephalus Salter, 1865 ; Mon. Brit. Tril., p. 113, pi. 11, figs. 1-10. 
 
 delphinocephalus Hall, 1883; 12th Ann. Rept. Dept. Geol. Nat. Hist. Indiana, 
 
 1882, p. 332, pi. 34, figs. 17, 18. 
 
 delphinocephalus ? Hall, 1875 ; 28th Rept. New York State Mus. Nat. Hist., pi. 
 
 34, figs. 17, 18. 
 
 delphinocephalus Hall, 1879 ; 28th Rept. New York State Mus. Nat. Hist., p. 187, 
 
 pi. 32, figs. 17, 18. 
 
 [Trimerus] jacksoni Green, 1837 ; Am. Jour. Sci., 1st series, vol. 32, p. 347. 
 
 Devonian. 
 
 major Whitfield, 1885 ; Bull. Am. Mus . Nat. Hist., vol. 1, No. 6, p. 193, pi. 22. 
 
 Oriskany. 
 
 major Hall, 1888 ; Pal. New York, vol . 7, p. 4, pi. 5 a, fig. 1. * 
 
 vanuxemi Hall, 1859 ; Pal. New York, vol. 3, p. 352, pi. 73, figs. 9-14. 
 
 Lower Helderberg. 
 
 vanuxemi Hall, 1888; Pal. New York, vol. 7, p. 11, pi. 5 b, figs. 1,2. 
 
 Hopolichas Dames, 1877; Zeitschr. Deutsch. geol. Gesell., 1872, p. 794. 
 
 Type, Licha8 ( Hopolichas ) tricuspidata Beyricli. 
 
 Illaenurus Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 176. 
 
 Type, Illcenurus quadratus Hall. 
 
 convexus Whitfield, 1878; Ann. Rept. Geol. Survey Wisconsin, 1877, p. 66. 
 
 ♦ Lower Magnesian. 
 
 convexus Whitfield, 1882 ; Geol. Wisconsin, vol. 4, p. 203, pi. 4, figs. 3-5. 
 
 eurekensis Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 97, pi. 12, figs. 4, 4 a. Pogonip. 
 
V0GDE6.J 
 
 CATALOGUE OF TRILOBITES. 
 
 119 
 
 Illaenurus quadratus Hall, 1863 ; 16tli Kept. New York State Cab. Nat. Hist., p. 176, 
 pi. 7, figs. 52-57. Potsdam. 
 
 Illaenus Dalman, 1826 ; Palraad., p. 50. 
 
 Type, Illcenus crassicauda, Wahl., Nova Acta Soc. Scient. Upsal., vol. 8, p. 8, pi. 2, 
 figs. 5, 6 (not pi. 7, figs. 5, 6, Illcenus esmarki ). 
 
 Syn., Actinolobus Eichwald, 1860. 
 
 Alceste Corda, 1847. 
 
 Cryptonymus Eichwald, 1825 (in part), not Cryptonymus Eichwald, 1840. 
 Deucalion Stochegloff, 1827. 
 
 JEclillcenus Salter, 1866 (subgenus). 
 
 Hydrolcenus Salter, 1866 (subgenus). 
 
 U lamopsis Salter, 1865 (subgenus). 
 
 Octillcenus Salter, 1866 (subgenus). 
 
 Thaleops Conrad, 1843. 
 
 ambiguus Foerste, 1885 ; Bull. Denison Univ., vol. 1, p. 106, pi. 14, figs. 9 a, b ; 
 
 fig. 10 a, b, c ; fig. 11. Clinton. 
 
 ambiguus Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 94. 
 
 ambiguus Foerste, 1886; 15th Ann. Rept. Geol. Nat. Hist. Survey Minnesota, p. 
 
 480, fig. 3. 
 
 americanus Billings, 1859 ; Canadian Naturalist, vol. 4, p. 371. Trenton. 
 
 americanus Billings, 1865 ; Pal. Foss., vol. 1, p. 329, fig. 316 a-d ; fig. 318. 
 
 angusticollis Billings, 1859 ; Canadian Naturalist, vol. 4, p. 377, fig. 10 a-d. 
 
 Trenton. 
 
 arcturus Hall, 1847 ; Pal. New York, vol. 1, p. 23, pi. 4 Ms, fig. 12. 
 
 Chazy and Trenton. 
 
 arcturus Emmons, 1855 ; Am. Geology, vol. 1, pt. 2, p. 235, pi. 3, fig. 12. 
 
 arcturus (Hall) Billings, 1859 ; Canadian Naturalist, vol. 4, p. 379. 
 
 arcturus Billings, 1865 ; Pal. Foss., vol. 1, p. 279, fig. 265. 
 
 armatus Hall, 1867; 20th Rept. New York State Cab. Nat. Hist., p. 330, pi. 22, 
 
 figs. 1.2. Niagara. 
 
 armatus Hall, 1870 ; 20th Rept. New York State Cab. Nat. Hist., p. 418, pi. 22, 
 
 figs. 1, 2 ; pi. 25, fig. 22. 
 
 armatus? Hall, 1875 ; 28th Rept. New York State Mus. Nat. Hist., pi. 32, figs. 
 
 19, 20. 
 
 armatus? Hall, 1879 ; 28th Rept. New York State Mus. Nat. Hist., p. 189, pi. 32, 
 
 figs. 19, 20. 
 
 armatus Hall, 1883 ; 12th Ann. Rept. Dept. Geol. Nat. Hist. Indiana, 1882, p. 335, 
 
 pi. 34, figs. 19, 20 ; pi. 33, fig. 12. 
 
 barriensis (Murch.) Hall; Trans. Albany Inst., vol. 4, p. 227; abstract, p. 33, 
 
 May, 1863. 
 
 barriensis (Murch.) Roemer, 1860; Die sil. Fauna W. Tennessee, p. 83, pi. 5, 
 
 fig. 23. Niagara. 
 
 \_Bumastm'] barriensis (Murch.), 1839; Sil. Syst., p. 656, pi. 7 Ms, figs. 3 a-d, 
 
 pi. 14, fig. 7 (in part). 
 
 barriensis Salter, 1859 ; Murchison’s Siluria (2d. ed.), pi. 17, figs. 9-11. 
 
 bayfieldi Billings, 1859 ; Canadian Naturalist, vol. 4, p. 369, figs. 4-6. Chazy. 
 
 clavifrons Billings, 1$59 ; Canadian Naturalist, vol. 4, p. 379. 
 
 Chazy and Trenton. 
 
 conifrons Billings, 1859 ; Canadian Naturalist, vol. 4, p. 378, figs. 7-9. Trenton. 
 
 conradi Billings, 1859; Canadian Naturalist, vol. 4, p. 372, figs. 7-9. (See Pan- 
 
 deria conradi.) Trenton. 
 
 consimilis Billings, 1865; Pal. Foss., vol. 1, p. 277, figs. 263 a-c ; p. 331, fig. 317. 
 
 Compare Ilhenus esmarki Schlotheim. Quebec. 
 
 consobrinus Billings, 1865; Pal. Foss., vol. 1, p. 280, fig. 268; p. 332, fig. 320. 
 
 Quebec. 
 
[BULL. 63. 
 
 120 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Illaenus cornigerus Hall, 1872; 24tli Rept. New York State Cal). Nat. Hist., p. 186, 
 pi. 13, tigs. 20, 21. Clinton. 
 
 [j Entomo8tracetes~\ crassicauda Wahlenberg, 1821; Nova Acta Soc. Scieut. Upsal., 
 
 vol. 8, p. 27, pi. 2, figs. 5, 6 (not pi. 7, figs. 5, 6). 
 
 crassicauda Holm, 1882; Svenska Vet.-Akad. Handl., vol. 7, No. 3, pi. 2, 
 
 figs. 21-27. 
 
 crassicauda ? Hall, 1847 ; Pal. New York, vol. 1, p. 24, pi. 4 bis, fig. 13; pi. 60, 
 
 figs. 4 a-d. 
 
 crassicauda (Wahl.) Meek and Wortken, Geol. Survey Illinois, vol. 3, p. 322, 
 
 pi. 3, figs. 1 a-1 b. 
 
 Compare Illcenus consimilis and I. esmarckii. 
 
 cuniculus Hall, 1867 ; 20th Rept. New York State Cab. Nat. Hist., p. 377, pi. 22, 
 
 fig. 12. Niagara. 
 
 cuniculus Hall, 1870 ; 20th Rept. New York State Cab. Nat. Hist., p. 421, pi. 22, 
 
 fig. 12 (rev. ed.). 
 
 daytonensis Hall and Whitfield, 1875 ; Pal. Ohio, vol. 2, p. 119, pi. 5, figs. 14-16. 
 
 Ciinton. 
 
 daytonensis Foerste, 1885; Bull. Denison Univ., vol. 1, p. 104, pi. 14, figs. 4 a, 
 
 b ; figs. 6, 7, 7 a, b, c. 
 
 daytonensis Foerste, 1887; Bull. Denison Univ., vol. 2, p. 93, pi. 8, figs. 1-7. 
 
 fraternus Billings, 1865; Pal. Foss., vol. 1, p. 276, figs. 262 a, b. Quebec. 
 
 globosus Billings, 1859 ; Canadian Naturalist, vol. 4, p. 367, figs. 1-3. Cliazy. 
 
 [ Bumastus ] graftonensis Meek and Worthen, 1870; Proc. Acad. Nat. Sci.Phila., 
 
 p. 54. 
 
 [Rumasfus] graftonensis Meek and Worthen, 1875; Geol. Survey Illinois, vol. 
 
 6, p. 508, pi. 25, fig. 4. 
 
 grandis Billings, 1859 ; Canadian Naturalist, vol. 4, p. 380. Hudson River. 
 
 — — herricki Foerste, 1886; 15th Ann. Rept. Geol. Nat. Hist. Minnesota, p. 479, 
 * fig. 2. Trenton. 
 
 imperator Hall, 1861 ; Rept. Progress Geol. Survey Wisconsin, p. 49. Niagara. 
 
 imperator Hall, 1867 ; 20th Rept. New York State Cab. Nat. Hist., p. 332, pi. 22, 
 
 figs. 15-17; pi. 2.3, figs. 2 : 3. 
 
 imperator Hall, 1870; 20th Rept. New York State Cab. Nat* Hist., p. 420, pi. 
 
 22, figs. 15-17 ; pi. 23, figs. 2, 3. 
 
 imperator Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 306, pi. 21, figs. 4,5. 
 
 incertus Billings, 1865; Pal. Foss., vol. 1. p. 332, fig. 319. Quebec. 
 
 * indeterminatus Walcott, 1877 ; Advanced sheets 31st Rept. New York State 
 
 Mus. Nat. Hist.,p. 19. Trenton. 
 
 indeterminatus Walcott, 1879 ; 31st Rept. New York State Mus. Nat. Hist., p. 70. 
 
 insignia Hall, 1867 ; 20th Rept. New York State Cab. Nat. Hist., p. 331, figs. 5, 
 
 6, pi. 22, figs. 13, 14. 
 
 [ Bumastus ] insignis Salter, 1867 ; Mon. Brit. Tril., p. 207. 
 
 insignis Hall, 1867 ; 20th Rept. New York State Ca"b. Nat. Hist., p. 331, figs. 5, 6; 
 
 pi. 22, figs. 13, 14. 
 
 insignis Hall, 1870; 20th Rept. New York State Cab. Nat. Hist.; p. 419, figs. 10, 
 
 11 ; pi. 22, figs. 13, 14. 
 
 [ Bumastus ] insignis Meek, 1873 ; Pal. Ohio, vol. 1, jh 189, pi. 15, figs. 5 a-c. 
 
 insignis Holm, 1882; De Svenska Art. Tril. Illsenus, p. 127. 
 
 insignis Whitfield, 1882 ; Geol. Wisconsis, vol. 4, p. 305, pi. 21, figs. 6-10. 
 
 insignis Foerste, 1886; 15th Ann. Rept. Geol. Nat. Hist. Survey Minnesota', p. 
 
 481. 
 
 ioxus Hall, 1867 ; 20tli Rept. New York State Cab. Nat. Hist., p. 378, pi. 22, figs. 
 
 4-10. Niagara. 
 
 IBumastus'] ioxus Hall, 1870; 20th Rept. New York State Cab. Nat. Hist., p. 
 
 420, pi. 22, figs. 4-10. 
 
VOGDES.J 
 
 CATALOGUE OF TRILOBITES. 
 
 121 
 
 Illaenus [ Bumastus ] ioxus Hall, 1883; 12tli Ann. Rept. Dept. Geol. Nat. Hist. In- 
 diana, 1882, p. 335, pi. 38, figs. 13, 14. 
 
 ioxus Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 304, pi. 21, figs. 11, 12. 
 
 [ Bumastus ] ioxus Hall, 1883 ; Trans. Albany Inst., vol. 10, p. 76. 
 
 latidorsata Hall, 1847 ; Pal. New York, vol. 1, p. 230, pi. 60, figs. 6 a, b. Trenton. 
 
 madisonianus Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 307, pi. 20, figs. 8,9. 
 
 Niagara. 
 
 madisonianus Foerste, 1885; Bull. Denison Univ., vol. 1, p. 106, pi. 14, figs. 1 
 
 a, b and 2 a, b. 
 
 madisonianus Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 93, pi. 8, figs. 8-10. 
 
 Clinton. 
 
 milleri Billings, 1859; Canadian Naturalist, vol. 4, p. 375, fig. 10. Trenton. 
 
 milleri Walcott, 1877 ; Advance sheets 31st Rept. N. Y. State Mus. Nat. Hist., 
 
 p. 20. 
 
 milleri Walcott, 1879 ; 31st Rept. N. Y. State Mus. Nat. Hist., p. 71. 
 
 [A 7 iZews] minnesotensis Foerste, 1886 ; 15th Ann. Rept. Geol. Minnesota, p. 478, 
 
 fig. 1. Trenton. • 
 
 niagarensis Whitfield, 1880 ; Ann. Rept. Geol. Wisconsin, 1879, p. 69. Niagara. 
 
 Name changed, by request of the Wisconsin Geological Survey, from Illcenus 
 niagarensis to Illaenus madisonianus. Explanation omitted by accident in 
 the Final Report Pal. Wisconsin, p. 307. 
 
 orbicaudatus Billings, 1859; Canadian Naturalist, vol. 4, p. 379. Hudson. 
 
 [ Thaleops ] ovatus Conrad, 1843; Proc. Acad. Nat. Sci. Phila., vol. 1, p. 332. 
 
 Trenton. 
 
 [ Tlialeops (Illcenus)] ovatus Hall, 1847 ; Pal. New York, vol. 1, p. 259, pi. 67, figs- 
 
 6 a-b. 
 
 ovatus Whitfield, 1882 ; Geol. Wisconsin, vol. 4, p. 238, pi. 5, figs. 1, 2. 
 
 pomatia Salter, 1867 ; Mon. Brit. Tril., pi. 27, figs. 6, 7. 
 
 pterocephalus Whitfield, 1878 ; Ann. Rept. Geol. Wisconsin, 1877, p. 87. 
 
 Niagara. 
 
 pterocephalus Whitfield, 1882 ; Geol. Wisconsin, vol. 4, p. 309, pi. 20, figs. 10-12. 
 
 simulator Billings, 1865 ; Pal. Foss., vol. 1, p. 337, figs. 315 a, b. Quebec. 
 
 taurus Hall, 1861 ; Rept. Prog. Geol. Survey Wisconsin, p. 49. Niagara. 
 
 taurus Meek and Worthen, 1865 ; Geol. Survey Illinois, vol. 3, p. 320, pi. 3, fig. 2. 
 
 [ Bumastus ] trentonensis Emmons, 1842 ; Geol. New York, 3d Geol. Dist.,p. 390 
 
 fig. 1. Trenton. 
 
 [Bumastus] trentonensis, 1854 ; 7th Rept. New York State Cab. Nat. Hist., p. 64, 
 
 fig. 1. 
 
 [ Bumastus ] trentonensis Emmons, 1855; Am. Geology, vol. 1, pt. 2, p. 215, pi. 15, 
 
 fig. 13. 
 
 trentonensis Hall, 1847 ; Pal. New York, vol. 1, p. 230, pi. 60, fig. 5. 
 
 tumidifrons Billings, 1865 ; Pal. Foss., vol. 1, p. 278, fig. 264. Quebec. 
 
 vindex Billiugs, 1865 ; Pal. Foss., vol. 1, p. 179, fig. 160. Cliazy. 
 
 [Bumastus] worthenanus Winchell and Marcy, 1866; Mem. Boston Soc. Nat. 
 
 Hist., vol. 1, pt. 1, p. 105, pi. 3, fig. 13 (referred by Hall, 20th Rept. New York 
 State Cab. Nat. Hist., to Illcenus armatus Hall). 
 l8oletu8 De Kay, 1825; Annals Lyceum Nat. Hist. New York, vol. 1, p. 174. 
 
 canalis. (See Asaphus canalis.) 
 
 cgclop8. (See Asaphus platycephalus.) 
 
 gigas. (See Asaphus platycephalus.) 
 
 maximu8. (See Asaphus maximus.) 
 
 megalops Green, 1832; Mon. Tril. N. A., p. 70, cast 7b. 
 
 megistos. (See Asaphus maximus.) 
 
 platycephalus. (See Asaphus platycephalus.) • 
 
 planus. (See Asaphus platycephalus.) 
 
122 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63 . 
 
 Isolelus stegops. (See Asaphus platycephalus. ) 
 
 vigilans, (See Asaphus vigilans.) 
 
 Lichas Dalman, 1826; Palsead., pp. 53, 71, pi. 6, fig. 1. 
 
 Type, Lichas laciniatus Wahlenberg. 
 
 Syn., Platynotus Conrad, 1838; Geol. Survey New York, Rept. Pal. Dept., p. 118. 
 Arges Goldfuss, 1839 (in part). 
 
 Metopias Eichwald, 1842 ; Die Urwelt Russ., p. 62, pi. 3, figs. 21-23. 
 Actinurus Castelnau, 1843; Syst. Sil. de FAm6r.,p. 21. 
 
 Nuttainia Portlock and Emrurich. 
 
 Corydocephalus Corda, 1847 ; Prodr., p. 255. 
 
 Dicranopeltis Corda, 1847 ; Prodr., p. 257. 
 
 Acanthopyge Corda, 1847 ; Prodr., p. 260. 
 
 Dicranoymas Corda, 1847; Prodr., p. 261. 
 
 Subgenera, Hoplolichas Dames, 1877; Zeitscbr. Deutsch. geol. Gesellsch., 1877, p. 
 794. 
 
 Type, Hoplolichas tricuspidata Beyrich. 
 
 Conolichas Dames, 1877; Zeitschr. Deutscli. geol. Gesellsch., 1877, p. 806. 
 Type, Conolichas cequiloha Steinhardt. 
 
 armatus Hall. (See Acidaspis eriopis Hall.) 
 
 bigsbyi Hall, 1859 ; Pal. New York, vol. 3, p. 364, pi. 77, figs. 1-8. 
 
 Lower Helderberg. 
 
 1 Conolichas'] bigsbyi ? Hall, 1888 ; Pal. New York, vol. 7, p. 80, pi. 19 a, fig. 1. 
 
 [ Paradoxides ] boltoni Bigsby, 1825; Jour. Acad. Nat. Sci. Phila., vol. 4, p. 365, 
 
 plate. Niagara. 
 
 [ Paradoxides ] boltoni Green, 1832 ; Monthly Am. Jour. Geol., etc., vol. 1, p. 560, 
 
 pi. 1, fig. 5. 
 
 [ Paradoxides ] boltoni Green, 1832; Mon. Tril. North America, p. 60, pi. 1, fig. 5. 
 
 [ Paradoxides ] boltoni Harlan, 1834 ; Trans. Geol. Soc. Penn., vol. 1, p. 103. 
 
 [ Paradoxides ] boltoni Harlan, 1835; Med. and Phys. Researches, p. 303. 
 
 \_Plaiynotus] boltoni Conrad, 1838 ; Rept. Pal. Dept. Geol. Survey New York, 
 
 p. 118. 
 
 [ Actinurus] boltoni Castelnau, 1843 ; Syst. Sil. de TAm6r., p. 21, pi. 3, fig. 3. 
 
 boltoni Hall, 1852 ; Pal. New York, vol. 2, p. 311, pi. 69 ; pi. 70, figs. 1 a-i. 
 
 boltoni Meek and Worthen, 1875; Geol. Survey Illinois, vol. 6, p. 508, pi. 25, 
 
 fig. 5. 
 
 boltoni var. occidentalis Hall, 1863; Trans. Albany Inst., vol. 4, p. 223; ab- 
 stract, p. 29. 
 
 boltoni var. occidentalis Hall, 1875 ; 28th Rept. New York State Mus. Nat. 
 
 Hist. Expl., p. 34, figs. 8-11. 
 
 boltoni var. occidentalis Hall, 1879; 28tli Rept. New York State Mus. Nat. 
 
 Hist., p. 198, pi. 34, figs. 8-11. 
 
 boltoni var. occidentalis Hall, 1883 ; 12th Ann. Rept. Dept. Geol. Nat. Hist. 
 
 Indiana, 1882, p. 334, pi. 36, figs. 8, 11, 12 (?). 
 
 breviceps Hall, 1863 ; Trans. Albany Inst., vol. 4, p. 222; abstract, p. 28. 
 
 Niagara. 
 
 breviceps Hall and Whitfield, 1875 ; Pal. Ohio, vol. 2, p. 156, pi. 6, fig. 17. 
 
 breviceps Hall, 1875; 28th Rept. New York State Mus. Nat. Hist. Expl., pi. 34, 
 
 figs. 1-7. 
 
 breviceps Hall, 1879 ; 28th Rept. New York State Mus. Nat. Hist., p. 197, pi. 34, 
 
 figs. 1-7. 
 
 breviceps Hall, 1883; 12th Ann. Rept. Dept. Geol. Nat. Hist. Indiana, 1882, p. 
 
 343, pi. 36, figs. 1-7. 
 
 breviceps Foerste, 1885 ; Bull. Denison Univ., vol. 1, p. 112, pi. 13, figs. 2, 6 a, b. 
 
 Clinton. 
 
vogdesI CATALOGUE OF TRILOBITES. 123 
 
 Liclias breviceps Foerste, 1837 ; Bull. Denison Univ., vol. 2, p. 98, pi. 8, figs. 18, 19. 
 Not Lichas breviceps Hall, 1867 ; 20tli Rept. New York State Cab. Nat. Hist., p. 
 377, pi. 21, figs. 12-14; also rev. ed., p. 424, pi. 21, figs. 12-14. (See Liclias 
 emarginatus.) 
 
 canadensis Billings, 1866; Catalogue Sil. Foss. Anticosti, p. 65, fig. 22. 
 
 champlainensis Whitfield, 1886; Bull. Am. Mus. Nat. Hist. New York, vol. 1, No. 
 
 8, p. 342, pi. 23, figs. 6-8. Birdseye. 
 
 [ Arges ] contusus Hall, 1888 ; Pal. New York, vol. 7, p. 83, pi. 19 b, figs. 3-6. 
 
 Upper Helderberg. 
 
 cucullus Meek and Worthen, 1865 ; Proc. Acad. Nat. Sci. Phila., p. 266. 
 
 Trenton. 
 
 cucullus Meek and Worthen, 1866; Geol. Survey Illinois, vol. 3, p. 299, pi. 1, 
 
 figs. 6 a-c. 
 
 decipiens Winchell and Marcy, 1866; Mem. Boston Soc. Nat. Hist., vol. l,pt. 1, 
 
 p. 104, pi. 3, fig. 11. Niagara. 
 
 [ Ceratolichas ] dracon Hall, 1888 ; Pal. New York, vol. 7, p. 85, pi. 19, figs. 14-17. 
 
 Hall, 1876; Ulus. Devonian Foss. Crust., pi. 19, figs. 2, 3. Upper Helderberg. 
 
 emarginatus Hall, 1879; 28th Rept. New York State Mus. Nat. Hist., p. 199. 
 
 .Niagara. 
 
 Syn., Lichas breviceps Hall; 20th Rept. New York State Cab. Nat. Hist., p. 377, 
 pi. 21, figs. 12-14, rev. ed., p. 424, pi. 21, figs. 12-14. 
 
 eriopis, Hall. Upper Helderberg. 
 
 Syn., Lichas armatus Hall, 1861 ; Des. New Species Foss., p. 81. 
 
 Liclias armatus Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 
 109. 
 
 eriops Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 226. 
 
 [ Acidaspis ( Terataspis )] eriops Hall, 1876; Illus. Devonian Foss. Crust., pi. 19, 
 
 figs. 4-7,10, 11. 
 
 [ Acidaspis (Terataspis?) ] sp. ? Hall, 1876; Illus. Devonian Foss. Crust., pi. 19, 
 
 fig. 12. 
 
 [ Conolichas ] eriops Hall, 1888; Pal. New York, vol. 7, p. 78, pi. 19 a, figs. 2-13, 
 
 15, 16. 
 
 grandis Hall, 1861 ; Des. New Species Foss., p. 82. Upper Helderberg. 
 
 grandis HalJ, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 110. 
 
 grandis Hall, 1863 ; 16th Rept. New York State Cab. Nat. Hist., i>. 223. (Sub- 
 genus Terataspis.) 
 
 Syn., superbus Billings, 1875; Canadian Naturalist, vol. 7, p. 239. 
 
 [ Acidaspis ( Terataspis )] grandis Hall, 1876; Illus. Devonian Foss. Crust., pis. 
 
 17, 18. 
 
 [Terataspis] grandis Hall, 1888; Pal. New York, vol. 7, p. 73, pi. 17, figs. 1-6; 
 
 pi. 1*, figs. 1,2; pi. 19, figs. 1-7. 
 
 [ Ceratolichas ] grandis Hall, 1888; Pal. New York, vol. 7, p. 84, pi. 19 b, figs. 
 
 7-13. 
 
 [ Ceratolichas ] gryps Hall, 1888; Pal. New York, vol. 7, p. 84, pi. 19 b, figs. 
 
 7-13. 
 
 harrisi Miller, 1878; Jour. Cincinnati Soc. Nat. Hist., vol. 1, p. 106, pi. 3, fig. 9. 
 
 Hudson. 
 
 [ Acidaspis n. sp. ?] Hall, 1876; Illus. Devonian Foss. Crust., pi. 19, fig. 1 (not figs. 
 
 2,3). Upper Helderberg. 
 
 [ Conolichas ] hispidus Hall, 1888; Pal. New York, vol. 7, p. 77, pi. 19 a, ligs. 14, 
 
 17, 18. 
 
 Syn., [ Acidaspis ( Terataspis )] eriops Hall, 1876; Illus. Dev. Foss., pi. 19, figs. 8,9. 
 
 Upper Helderberg. 
 
 [Hoplolichas] hylaeus Hall, 1888; Pal. New York, vol. 7, p. 81, pi. 19 b, ligs. 1,2. 
 
 Upper Helderberg. 
 
 jukesi I3i lliugs, 1865; Pal. Foss., vol. 1, p. 282, fig. 260; also p. 335, fig. 323. 
 
 Quebec. 
 
124 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63. 
 
 Lichas minganensis Billings, 1865; Pal. Foss., vol. 1, p. 181, figs. 163 a, b. 
 
 Chazy and Trenton. 
 
 nereus Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 226. 
 
 Niagara. 
 
 obvius Hall, 1870; 20th Rept. New York State Cab. Nat. Hist., p. 424, pi. 25, 
 
 fig. 19- Niagara. 
 
 [ Calymene] phlyctanodes Green, 1837 ; Am. Jour. Sci., 1st series, vol. 32, p. 167. ' 
 
 Niagara. 
 
 [Arges] phlyctanodes Hall, 1852; Pal. New York, vol. 2, p. 314, pi. 70, figs. 
 
 2 a, c. 
 
 [ Dicranogmus] ptyonurus Hall, 1888 ; Pal. New York, vol. 7, p. 86, pi. 19 b, figs. 
 
 19-21. Niagara. 
 
 pugnax Winchell and Marcy, 1866 ; Mem. Boston Soc. Nat. Hist., vol. 1, pt. 1, 
 
 p. 103, pi. 3, fig. 10. Niagara. 
 
 pugnax Hall, 1867 ; 20th Rept. New York State Cab. Nat. Hist., p. 393 (rev. ed., 
 
 p. 424, pi. 25, tig. 20). 
 
 pustulosus Hall, 1859 ; Pal. New York, vol. 3, p. 366, pi. 77, figs. 9-12 ; pi. 78, 
 
 figs. 1-6, fig. 7 (T). Lower Helderberg. 
 
 puhtulosus Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 19, fig. 13. 
 
 [Conoliclias] pustulosus Hall, 1888; Pal. New York, vol. 7, p. 80, pi. 19, figs. 
 
 8 , 10 , 11 . 
 
 superbus Billings, 1875; Canadian Naturalist, n. s:, vol. 7, p. 239. (See Lichas 
 
 grandis.) Corniferous. 
 
 [ Asaphus? ] trentonensis Conrad, 1842; Jour. Acad. Nat. Sci. Phila., vol. 8, p. 
 
 277, pi. 16, fig. 16. Trenton. 
 
 [ Platynotus ] trentonensis Hall, 1847 ; Pal. New York, vol. 1, p. 235, pi. 64, figs. 
 
 1 a-e. 
 
 — - trentonensis Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 127. 
 
 Lloydia Vogdes, 1889 (generic name for Bathyurus bituberculatus Billings for its type). 
 Loganellus Devine, 1863 ; Canadian Naturalist, vol. 8, p. 95. (See Ptychoparia, 
 Crepicephalus, and Olenus.) 
 
 logani Devine, 1863; Canadian Naturalist, vol. 8, p. 95. (See Ptychoparia 
 
 logani.) 
 
 [Olenus?] logani Billings, 1865; Pal. Foss., vol. 1, p. 201, figs. 185, 186. 
 
 quebecensis Billings, 1865 ; Pal. Foss., vol. 1, p. 203. (See Ptychoparia logani.) 
 
 Lonchocephalus Owen, 1852; Rept. Geol. Survey Wisconsin, Iowa, and Minnesota, 
 p. 576. (See Anomocare hamulus (Owen) Dames.) 
 
 Megalaspis Angelin, 1852; Palseont. Scand., p. 15. 
 
 Type, Megalaspis gigas Ang., pi. 12, fig. 3. 
 
 belemnurus White, 1874 ; Rept .Invert. Foss., etc., p. 11. Quebec. 
 
 belemnurus White, 1877; Geog. Sur. W. 100th Meridian, Pal., vol. 4, p. 59, 
 
 pi. 3, fig. 9. 
 
 [Asaphus ( meglaspis )] goniocerus Meek, 1873; 6th Ann. Rept. Geol. Survey 
 
 Territories, 1872, p. 480. Quebec. 
 
 Menocephalus Owen, 1852) Rept. Geol. Survey Wisconsin, Iowa, and Minnesota, 
 p. 577. 
 
 Dr. D. D. Owen refers one species to this genus, Menocephalus mimiesotensis, 
 pi. 1, fig. 11, which has a highly arched and hemispherical glabella. 
 
 globosus Billings, 1860 ; Canadian Naturalist, vol. 5, p. 317, figs. 17-19. 
 
 Quebec. 
 
 globosus Billings, 1865 ; Pal. Foss., vol. 1, p. 408, figs. 388 a-c. 
 
 minnesotensis Owen, 1852 ; Rept. Geol. Survey Wisconsin, Iowa, and Minne- 
 sota,^. 577, pi. 1, fig. 11. Cambrian. 
 
 salteri Billings, 1863; Canadian Naturalist, vol. 8, p. 210, figure. Cambrian. 
 
 salteri Billings, 1865; Pal. Foss., vol. 1, p. 203, fig. 187. 
 
vogdes.] CATALOGUE OF TRILOBITES. 125 
 
 Menocephalus salteri ? Rominger, 1888; Proc. Acad. Nat. Sci. Phila., pi. 16, pi. 1, 
 fig. 6. 
 
 sedgwicki Billings, 1860 ; Canadian Naturalist, vol. 5, p. 316, fig. 16. Quebec. 
 
 sedgwicki Billings, 1865 ; Pal. Foss., vol. 1, p. 407, fig. 387. 
 
 Mesonacis Walcott, 1885; Am. Jour. Sci., 3d series, vol. 29, p. 329. 
 
 \_Olenu.8~\ vermontana Hall, 1859; 12th Rept. New York State Cab. Nat. Hist., 
 
 p. 60, figure. Cambrian. 
 
 [ Olenus ] vermontana Hall, 1859 ; Pal. New York, vol. 3, p. 527, figure. 
 
 [ Paradoxides'] vermonti Emmons, 1860; Manual Geology, p. 280 (note A). 
 
 [ Paradoxides ] vermontana Barrande, 1861 ; Bull. Soc. G6ol. France, 2d series, 
 
 vol. 18, p. 277, pi. 5, fig. 8. 
 
 [ Paradoxides ] vermontana Billings, 1861 ; Geology Vermont, vol. 2, p. 950. 
 
 \_Barrandia] vermontana Hall, 1861.; 13th Rept. New York State Cab. Nat. 
 
 Hist., p. 117, figure. 
 
 [ Barrandia ] vermontana Hall, 1861 ; Geol. Vermont, vol. 1, p. 370, pi. 13, figs. 
 
 2, 4, and 5. 
 
 [ Paradoxides ] vermontana Billings, 1863 ; Geol. Canada, p. 953. 
 
 [ Olenellus] vermontana Hall, 1862 ; 15th Rept. New York State Cab. Nat. Hist., 
 
 p. 114. 
 
 [ OleneUus ] vermontana Billings, 1865 ; Pal. Foss., vol. 1, p. 10. 
 
 [ Olenellus ] vermontana Whitfield, 1884; Bull. Am. Mus. Nat. Hist. New York, 
 
 vol. 1, p. 152, pi. 15, figs. 2-4. 
 
 vermontana Walcott, 1885; Am. Jour. Sci., 3d series, vol. 29, p. 329, figs. 1,2. 
 
 vermontana Walcott, 1885; Nature, vol. 32, p. 68. 
 
 vermontana Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 158, pi. 24, 
 
 figs. 1 a, b. 
 
 Microdiscus Emmons, 1855; Am. Geology, vol. 1, pt. 2, p. 116. 
 
 Type, Microdiscus speciosus Ford. 
 
 belli-marginatus Shaler and Foerste, 1888; Bull. Mus. Comp. Zool. Harvard 
 
 Coll., vol. 16, p. 35, pi. 2, fig. 19. Cambrian. 
 
 connexus Walcott, 1887 ; Am. Jour. Sci., 3d series, vol. 34, p. 194, pi. 1, figs. 4-4 b. 
 
 Cambrian. 
 
 dawsoni Hartt, 1868; Acadian Geology, p. 654, fig. 228. St. John. 
 
 Mr. Hartt originally described this species under the new generic name of 
 Daivsonia, but on Mr. E. Billings’s authority the species was referred to Micro- 
 discus in the Acadian Geology. 
 
 dawsoni Whiteaves, 1878; Am. Jour. Sci., 3d series, vol. 16, p. 225. 
 
 dawsoni Walcott, 1884; Bull.-U. S. Geol. Survey, No. 10, p. 23, pi. 2, figs. 3, 3 a. 
 
 [Agnostus] lobatus Hall, 1847 ; Pal. New York, vol. 1, p. 258, pi. 67, figs. 5 a-f. 
 
 Potsdam. 
 
 [Agnostus] lobatus Rogers, 1858; Geol. Survey Pennsylvania, vol. 2, p. 820, 
 
 fig. 614 (1-4). 
 
 lobatus Ford, 1873; Am. Jour. Sci., 3d series, vol. 6, p. 135 (foot-note). 
 
 lobatus Walcott, 1886 j’Bull. U. S. Geol. Survey, No. 30, p. 156, pi. 16, figs. 1, 1 a, b. 
 
 lobatus Shaler and Foerste, 1888; Bull. Mus. Comp. Zool. Harvard Coll., vol. 
 
 16, p. 36, pi. 2, fig. 13. 
 
 meeki Ford, 1876; Am. Jour. Sci., 3d series, vol. 11, p. 371. Lower Potsdam. 
 
 meeki Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 155, pi. 16, fig. 4. 
 
 parkeri Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 157, pi. 16, figs. 2, 2 a. 
 
 Middle Cambrian. 
 
 pulchellus (Hartt MS.) Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 24. 
 
 St. John. 
 
 punctatus Salter, 1864 ; Quart. Jour. Geol. Soc. London, vol. 20, p. 237, pi. 13, 
 
 n - St. John! 
 
 punctatus Whiteaves, 1878; Am. Jour. Sci., 3d series, vol. 16, p. 225. 
 
[BULL. 63 . 
 
 126 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Miciodiscus punctatus Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 24, pi. 2, 
 
 figs. 1, 1 a-c. 
 
 quadricostatus Emmons, 1855 ; Am. Geology, vol. 1, pt. 2, p. 116, pi. 1, fig. 8. 
 
 Taconic. 
 
 quadricostatus Emmons, 1860; Manual Geology, p. 88, fig. 73. 
 
 quadricostatus Barrande, 1861; Bull. Soc. Gdol. France, 2d series, vol. 18, p. 
 
 280, pi. 5, figs. 13 a, b. 
 
 speciosus Ford, 1873 ; Am. Jour. Sci., 3d series, vol. 6, p. 137, figs. 2 a, b. 
 
 Potsdam. 
 
 speciosus Ford, 1877 ; Am. Jour. Sci., 3d series, vol. 13, p. 147. 
 
 speciosus Ford, 1879 ; New York Tribune Extra, Sept. 2, 18/9, fig. 2. 
 
 speciosus Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 154, pi. 16, figs. 3, 
 
 3 a— c. 
 
 Nileus Dalman, 1826 ; Palaead., p. 246 (German trans., p. 49). 
 
 Type, Nileus armadillo Dalman. 
 
 affinis Billings, 1865; Pal. Foss., vol. l,p. 275, figs. 261 a, b. Quebec. 
 
 macrops Billings, 1865; Pal. Foss., vol. 1, p. 273, fig. 259. Quebec. 
 
 scrutator Billings, 1865; Pal. Foss., vol. 1, p. 274, fig. 260. Quebec. 
 
 Nuttania Eaton, 1832 (in part) ; Geological Text Book, p. 33. (See Trinucleus and 
 Homalojiotus. ) 
 
 concentrica Eaton, 1832; Geological Text Book, p. 34, pi. 1, fig. 2. 
 
 sparsa Eaton, 1832; Geological Text Book, p. 34. 
 
 Odontoceplialus Conrad, 1840 ; 3d Ann. Rept. Pal. Dept. New York Geol. Survey, p. 204. 
 
 IDalmanites ( Odontoceplialus )] Hall and Clarke, 1888; Pal. New York, vol. 7, 
 
 p. xxxiii. m 
 
 I can not do justice to this genus without giving a brief historical sketch, 
 which dates back to 1781. During this year M. T. Briinnich (Beskrivelse over 
 Trilobiten, Nye Samling af det Kong. Danske Yidensk. Skrifter, vol. 1, p. 392, 
 pi. 0, figs. 1 , 2) published a description of a fossil Trilobite from Coalbrook Dale 
 under the name of Trilobus caudatus. As this Trilobite in after years had many 
 generic names, I give a translation of the original description for the use 
 of students. The author figures the head and pygidium of Trilobus caudatus 
 and remarks: “As I was not fortunate enough to obtain a complete speci- 
 men of the entirely unknown fossil, but only broken parts, I can not distinctly 
 describe its size or number of rings; however, the annexed figures show 
 the distinct features of this species and their peculiar morphology. The size 
 of the fossil at its anterior bend is If inches, the front piece outside of the 
 crust is £ inch, its total length 34 inches; the broken back part, consisting 
 of about sixteen rings, is 1 inch in length to the tail, the latter being 1 inch 
 long. The head shield is surrounded by a flat-shaped edge, which terminates 
 in an upright protuberance with a tongue rounded anteriorly. The shell 
 shows various elevations separated by transverse furrows. The eyes on the 
 side of the shell are very protruding, semilunar in form, and faceted after the 
 eyes of insects. On the head-shield may be seen some small nodes, which 
 are also visible on the first ring and on some of the others. The tail di- 
 minishes in breadth and terminates in a narrow, long, and pointed projec- 
 tion. 
 
 The first systematic writer (Brongniart, Crust. Foss., p. 22) included this 
 species under his genus Asaphus, and it was so classified until 1844, when Dr. H. 
 F. Emmrich (Zur Morphologic der Trilobiten, p. 15, pi. 1, fig. 1) proposed the new 
 generic term of Dalmania for it. Unfortunately this term was then preoccupied 
 for a genus of the Diptera. Dr. H. F. Emmrich’s work was well known in 
 Europe, having appeared in two separate German editions, and also in English 
 (Scient. Mem., vol. 4, pt. 14, 1847). 
 
 In the year 1847 A. J. C. Corda (Prodr., p. 208, pi. 5, fig. 56) changed Eimnrich’s 
 generic name to Odontochile, a preoccupied term in natural history. This name 
 
V0GDE8.] 
 
 CATALOGUE OF TRILOBITES. 
 
 127 
 
 was only used by one other author (McCoy, Annals Nat. Hist., London, vol. 4, 
 1849), all others using Dalmania or its modified form, Dalmanites (Barrande). 
 
 In 1840 Milne-Ed wards (Crust., pp. 306,339) proposed the name of Pleura- 
 canthus for Calymene arachnoides Goldfuss, and Dr. Goldfuss that of Acaste 
 (Neues Jahrbuch fiir Mineral., 1843, p. 511) for such forms as Calymene dozening ice 
 Murch. 
 
 In America a typical species ( Dalmanites limulurus ) has been classed by all 
 American writers either under Dalmania or its modified form, but other species 
 properly of this geuus — that is, if we do not desire to overburden generic classi- 
 fication — have been given new generic names. The first was an obscure fossil 
 • described by Dr. Jacob Green (Am. Jour. Sci., 1st series, vol. 32, p. 343) as Cry- 
 pheeus bootlii, a generic term preoccupied for a genus of the Coleoptera at the 
 time it was used by l)r. Green. The second species consists of a poorly figured 
 tail, described and figured by Prof. Amos Eaton (Geological Text Book, p. 31, 
 pi. 1, fig. 1) as Asaphus selenurus, and by Dr. Jacob Green under the name of 
 Calymene odontocephala (Am. Jour. Sci., 1st series, vol. 25, p. 334). Prof. Amos 
 Eaton’s description was drawn from the tail of the fossil and Dr. Jacob Green’s 
 from the head. 
 
 Mr. T. A. Conrad in 1840 (3d Ann. Rept. Pal. Dept. New York Geol. Survey, p. 
 204) procured a perfect specimen of this Trilobite and united- the two species 
 under a new generic name. Odontoceplialus selenurus, taking Dr. Jacob Green’s 
 specific name for the genus, and that of Prof. Amos Eaton for the species. 
 
 The generic characteristics consist of a series of incisor-like denticulations 
 bordering the frontal margin of the head, and a pygidium with two terminal 
 spines. 
 
 Hall and Clarke (1888, Pal. New York, vol. 7, p. xxxiii) use the term as a 
 subgenus to Dalmanites. 
 
 If we follow the strict rule of priority and set aside the preoccupied name 
 Dalmania or Dalmanites for that of Odontoceplialus Conrad, we take for a generic 
 name a term indicating a denticulated cephalic shield, which is confined to a 
 special group and miscall such species as the well known type Dalmanites 
 caudatus. 
 
 We would therefore suggest, not only in honor of the learned Swedish author 
 on Trilobites, but also through courtesy, that the generic name of Dalmanites 
 
 be retained. 
 
 Odontoceplialus. (See Dalmanites [ Odonfocepnalus ] selenurus, D. [Odontoceplialus] 
 bifidens, D. [Odontoceplialus'] aegeria, and D. [Odontoceplialus] coronatus. 
 
 Ogygia Brongniart, 1822; Crust. Foss., p. 26. 
 
 Type, Asaphus buchii Brongniart, pi. 2, figs. 3 a-c. 
 
 [Asaphus] barrandi Hall, 1851; Rept. Geol. Lake Superior Land Dist. (Foster 
 
 and Whitney), pt. 2, p. 210, pi. 27, figs. 1 a-d ; pi. 28. Birdseye. 
 
 [Asaphus] barrandi Hall, 1862; Geol. Wisconsin, vol. 1, p. 41, fig. 4. 
 
 klotzi Rominger, 1887 ; Proc. Acad. Nat. Sci. Phila., p. 12, pi. 1, fig. 1. 
 
 Cambrian. 
 
 klotzi Walcott, 1888; Am. Jour. Sci., 3d series, vol. 36, p. 166. 
 
 [Ogyyi eH ] latissimus Eaton, 1832; Am. Jour. Sci., vol. 21, p. 136, foot-note. 
 
 [Ogyges] latissimus Eaton, 1832; Geol. Text Book, p. 33 (Homalonotus delphi- 
 
 nocephus). 
 
 parabola Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par., vol. 4, p. 245, pi. 
 
 2, fig. 35. Cambrian. 
 
 ? problematica Walcott, 1.884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 
 
 8, p. 63, pi. 10, figs. 2 a, b and 4. Cambrian. 
 
 producta Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par., vol. 4, p. 234, 
 
 pi. 2, figs. 31-34 ; also p. 245, pi. 2, fig. 35. Cambrian. 
 
 [Nio&e] producta Brogger, 1886; Om alderen af Olonellus zonm i Nordamerika, 
 
 p. 211. 
 
128 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 Ogygia [ Bathyuriscus ] productus Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 
 217, pi. 30, figs. 1, 1 a-i. 
 
 Syn., Ogygia parabola (H. & W.) Walcott, 1886; idem., p. 217. 
 
 serrata Romiuger, 1887 ; Proc. Acad. Nat. Sci. Pliila., p. 13, pi. 1, figs. 2, 2a. 
 
 Cambrian. 
 
 ? spinosa Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. >8, p. 
 
 63, pi. 9, fig. 22. (See Olenoides spinosa Walcott.) 
 
 vetustus Hall, 1847 ; Pal. New York, vol. 1, p. 227, pi. 60, fig. 1. Trenton. 
 
 vetustus Emmons, 1855; American Geology, vol. 1, pt. 2, p. 216, fig. 72. 
 
 Olenellus Hall, 1861; Des. N. Species of Foss., published in advance, 15tli Rept. 
 State Cab., p. 86. Hall, 1862 ; 15th Rept. State Cab. Nat. Hist. Albany, p. 114. 
 Type, Olenellus thompsoni Hall. 
 
 [ Elliptocephala ] asaphoides Emmons, 1844 ; Taconic System, p. 21, figs. 1-3. 
 
 Cambrian. 
 
 [ Elliptocephala ] asaphoides Emmons, 1846; Agric. New York, vol. 1, p. 65, figs. 
 
 1-3. 
 
 [ Olenus] asaphoides Hall, 1847 ; Pal. New York, vol. 1, p. 256, pi. 67, figs. 2 a, c. 
 
 [Olenus] asaphoides Fitch, 1849; Trans. N. Y. State Agric. Soc., vol. 9. p.865. 
 
 [ Elliptocephalus ] asaphoides Emmons, 1849; Proc. Am. Assoc. Adv. Sci., 1st 
 
 meeting, p. 18. 
 
 — — [Eliptocephalns] asaphoides Emmons, 1855 ; Am. Geology, vol. 1. pt. 2, p. 114, 
 figs. 1-3, pi. 1, fig. 18. 
 
 [ Paradoxides ] asaphoides Emmons, 1860; Manual Geology, pp. 87,280. 
 
 [Paradoxides] asaphoides Barrande, 1861; Bull. Soc. G6ol. France, 2d series, 
 
 vol. 18, p. 273, pi. 5, figs. 4, 5. 
 
 [Olenus] asaphoides Ford, 1871 ; Am. Jour. Sci., 3d series, vol. 2, p. 33. 
 
 [Elliptocephalus] asaphoides Ford, 1877 ; Am. Jour. Sci., 3d series, vol. 13, p. 
 
 266, plate, figs. 1-10. 
 
 [ Elliptocephalus ] asaphoides Ford ; Am. Jour. Sci., 3d series, vol. 15, p. 129. 
 
 asaphoides Ford, 1881 ; Am. Jour. Sci., 3d series, vol. 22, p. 250. 
 
 asaphoides Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 168, pi. 17, figs. 4, 
 
 8, 10 ; pi. 20, figs. 3, 3 a, b ; pi. 25, fig. 8. 
 
 gilberti (Meek MS.) White, 1874; Prelim. Rept. Invt. Foss. U. S. Geog. and 
 
 Geol. Survey West 100th Mer., p. 7. Potsdam. 
 
 [ Olenus] gilberti Gilbert, 1875 ; U. S. Geog. Survey West 100th Mer., vol. 3,^. 182. 
 
 gilberti White, 1877 ; U. S. Geog. Survey West 100th Mer., vol. 4, p. 44, pi. 2, figs. 
 
 1, 3 a-e. 
 
 gilberti Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 29, 
 
 pi 9, figs. 16, 16 a ; pi. 21, fig. 13. 
 
 gilberti Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 170, pi. 18, figs. 1, 1 
 
 a-c ; pi. 19, fig. 2, 2 a-k ; pi. 20, figs. 1, 1 a, 1 b, 4. 
 
 howelli (Meek MS.) White, 1874; Prelim. Rept. Invt. Foss. U. S. Geog. and 
 
 Geol. Survey West 100th Mer., p. 8. Potsdam. 
 
 [Olefins'] howelli Gilbert, 1875; U. S. Geog. Survey West 100th Mer., vol. 3, p. 
 
 183. 
 
 howelli White, 1877; U. S. Geog. Survey West 100th Mer., vol. 4, p. 47, pi. 2 f i 
 
 • figs. 4 a, b. 
 
 — » — howelli Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, pp. « 
 29, 30, pi. 9, figs. 15a-b, 16-16 a; pi. 21, figs. 1-9. 
 
 iddingsi Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. • 
 
 28, pi. 9, fig. 12. Cambrian. ^ 
 
 iddingsi Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 170, pi. 19, fig. 1. 
 
 [Paradoxides] macrocephalus Emmons, 1860; Manual Geology, p. 88, fig. 70. 
 
 [Olenus] thompsoni Hall, 1859; 12th Rept. New York State Cab. Nat. Hist., p. 
 
 57, figure. Cambrian, ) 
 
VOGDES.l 
 
 CATALOGUE OF TRILOBITES. 
 
 129 
 
 Olenellus [ Olenus ] thompsoni Hall, 1859 ; Pal. New York, vol. 3, p. 525, figure. 
 
 I Barr an dial thompsoni Hall, 1860 ; 13th Rept. New York State Cab. Nat. Hist., 
 
 p. 116, figure. 
 
 [ Paradoxides ] thompsoni Emmons, 1860 ; Mauual Geology, p. 280, note A. 
 
 [ Paradoxides] thompsoni Barrande, 1861 ; Bull. Soc. G6ol. France, 2d series, 
 
 vol. 18, p. 276, pi. 5, fig. 6. 
 
 [ Paradoxides ] thompsoni Billings, 1861 ; Geol. Vermont, vol. 2, p. 950. 
 
 [Barrandia] thompsoni Hall, 1861 ; Geol. Vermont, vol. 2, p. 369, pi. 13, fig. 1. 
 
 [ Paradoxides ] thompsoni Billings, 1861 ; Pal. Foss., vol. 1, p. 11 (pamphlet pub- 
 lished in advance). 
 
 thompsoni Hall, 1862; 15th Rept. New York State Cab. Nat. Hist, p. 114. 
 
 thompsoni Billings, 1863; Geol. Canada, p. 953. 
 
 [ Olenellus ] thompsoni Billings, 1865; Pal. Foss., vol. 1, p. 11. 
 
 thompsoni Whitfield, 1884; Bull. Am. Mus. Nat. Hist., New York, vol. l,p. 151 
 
 pi. 15, figs. 1-4. 
 
 thompsoni Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 167, pi. 17, figs. 
 
 1, 2, 4, 9 ; pis. 22, 23, figure. 
 
 vermontana. (See Mesonacis vermontana (Hall) Walcott.) 
 
 Olenoides Meek, 1877 ; U. S. Geol. Expl. 40th Par., Pal., vol. 4, p. 25. 
 
 Type, Olenoides nevadensis Meek. 
 
 fordi Walcott, 1887 ; Am. Jour. Sci., 3d series, vol. 34, p. 195, pi. 1, figs. 5, 5 b. 
 
 Cambrian. 
 
 flagricaudus. (See Zacanthoides flagricaudus.) 
 
 levis Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 187, pi. 25, figs. 3-3 a. 
 
 (See Zacanthoides levis.) Cambrian. 
 
 gothicus (Hall and Whitfield) Walcott. (See Dorypyge gothicus.) 
 
 ? marcoui Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 186, pi. 26, fig. 
 
 5-5 a, b. 
 
 [ Dikellocephalus ?] marcoui Whitfield, 1884 ; Bull. Am. Mus. Nat. Hist. New 
 
 York, vol. 1, p. 150, pi. 14, fig. 7. Cambrian. 
 
 [Paradoxides f ] nevadensis Meek, 1870 ; Proc. Acad. Nat. Sci. Phila., vol. 22, p. 62. 
 
 Middle Cambrian. 
 
 [Paradoxides?] nevadensis Meek, 1877 ; U. S. Geol. Expl. 40th Par., Pal., vol. 
 
 4, p. 23, pi. 1, fig. 5. 
 
 ifevadensis Meek, 1877 ; U. S. Geol. Expl. 40th Par., Pal., vol. 4, p. 25. 
 
 nevadensis Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 181, pi. 25, fig. 7. 
 
 nevadensis Walcott, 1888 ; Am. Jour. Sci., 3d series, vol. 36, p. 165. 
 
 Syn., Ogygia serrata (Rominger) Walcott, 1888; Am. Jour. Sci., 3d series, vol. 36, 
 
 p. 165. 
 
 [Olenoides] quadriceps (Hall and Whitfield) Walcott. (See Dorypyge quadri- 
 ceps.) 
 
 spinosus. (See Zacanthoides spinosus.) 
 
 tgpicali8. (See Zacanthoides typicalis.) 
 
 [ Dikellocephalm ] wahsatchensis Hall and Whitfield, 1877 ; U. S. Geol. Expl. 
 
 40th Par., Pal., vol. 4, p. 241, pi. 1, fig. 35. 
 
 wahsatchensis Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 189, pi. 29, 
 
 figs. 2,2 a. Middle Cambrian. 
 
 Syn., [Dikellocephalus?] gothicus (Hall and Whitfield) Walcott, 1886; Bull. U. S. 
 Geol. Survey, No. 30, p. 189. 
 
 wahsatchensis Walcott, 1888; Am. Jour. Sci., 3d series, vol. 36, p. 165. 
 
 Olenus Dalman, 1826 ; Pahead, p. 226. 
 
 Type, Olenus gibbosus Wahlcnberg. 
 
 asaphoides. (See Olenellus asaphoides.) 
 
 — ■ — holopyga. (See Bathynotus holopyga.) 
 
 logani. (See Ptychoparia logani.) 
 
 Bull. 03 9 
 
130 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63 . 
 
 Olenus thompsoni. (See Olenellus thompsoni.) 
 
 undulostriatus Hall, 1847 ; Pal. New York, vol. 1, p. 258, pi. 67, figs. 3 a,b. 
 
 Hudson. 
 
 utahensis Woodward, 1873 ; Rept. 43d Meeting Brit. Assoc. Adv. Sci. 
 
 utahensis Woodward, 1873; Geol. Mag., vol. 10, p. 523. Cambrian. 
 
 vermontana. (See IVlesonacis vermontana Hall.) 
 
 Oryctcocephalus Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 210. 
 
 primus Walcott, 188& ; Bull. U. S. Geol. Survey, No. 30, p. 210, pi. 29, figs. 3, 3 a. 
 
 Middle Cambrian. 
 
 Pagura Emmons, 1860 ; Manual Geology, p. 280. 
 
 Dr. E. Emmons uses this term in a subgeneric sense for Paradoxides [ Pagura ] 
 quadrispinosus. The note accompanying the Manual of Geology does not indi- 
 cate the author’s intentions with regard to the genus and new species. It was 
 probably intended for Paradoxides [ Peltura ] quadrispinosus, a synonym of in- 
 tended Peltara yOlenus'] holopyga Hall, 12th Rept. New York State Cab. Nat. 
 Hist., p. 61. Emmons figures this species on p. 80, fig. 57. 
 
 Fanderia Yolborth ; Mem. Acad. Sci. St.-Pdtersbourg, vol. 6, p. 31. 
 
 Type, Panderia triquetra Volb., pi. 3, fig. 13 bis, 17. 
 
 _ \IUoenu8-\ conradi Billings, 1859 ; Canadian Naturalist, vol. 4, p. 372, figs. 7-9. 
 
 L Trenton. 
 
 For other references, see Illcenus conradi Billings. 
 
 Paradoxides Brongniart, 1822; Crust. Foss., p. 30, pi. 4, fig. 1. 
 
 Type, Paradoxides tessini Brongniart. 
 
 Syn., Plutonia Salter, 1869; Quart. Jour. Geol. Soc. London, vol. 25, p. 52. 
 
 Plutonia sedgwicki, Quart. Jour. Geol. Soc. London, vol. 27, p. 399, pi. 15, 
 1~8. 
 
 acadicus Matthew, 1882; Trans. Roy. Soc. Canada, vol. 1, p. 103, pi. 9, figs. 
 
 16 18 Jol-in. 
 
 acadicus Matthew, 1884; Trans. Roy. Soc. Canada, vol. 2, p. 99, pi. 1, fig. 1. 
 
 acadicus Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 25, pi. 6, figs. 3-3 a. 
 
 arcuatus Harlan. (See Triarthrus beckii.) 
 
 barberi Winchell, 1884; 13th Rept. Geol. Nat. Hist. Survey Minn, p. 65, pi. 1, 
 
 „ _ Cambrian, 
 
 kg- 7 - , .. . 
 
 beckii. (See Triarthrus beckii.) _ « 
 
 bennetii Salter, 1859; Quart. Jour. Geol. Soc. London, vol. 15, p. 553, figure. 
 
 Cambrian. 
 
 _ bennetii Salter and Woodward, 1865; Chart of Foss. Crust., fig. 25. 
 
 })oltoni. (See Lidias boltoni.) , 
 
 decorus Billings, 1865; Pal. Foss., vol. 2, p. 75. 0 s ara * 
 
 eatoni. (See Triarthrus beckii.) 
 
 eteminicus Matthew, 1882 ; Trans. Roy. Soc. Canada, vol. 1, p. 92, pi. 9, 
 
 Yar. suricoides (figs. 4-6), var. breviatus , var. malicitus (fig. 13), var. pontifi- 
 cate (figs. 15, 15 a), var. quacoensis (figs. 14, 14 a). _ _ _ „ t 
 
 eteminicus Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 27, pi. 3, figs. 1- 
 
 harlani Green, 1834; Am. Jour. Sci., 1st series, vol. 35, p. 336. Cambrian. 
 
 harlani Green, 1835 ; Suppl. Mon. Tril. N. A., p. 14, cast 39. 
 
 harlani Rogers, 1856; Proc. Boston Soc. Nat. Hist., vol. 6, pp. 27,40. 
 
 harlani Stodder, 1856 ; Proc. Boston Soc. Nat. Hist., vol. 6, p. 369. 
 
 harlani Rogers, 1856; Am. Jour. Sci., 2d series, vol 22, p. 297 
 
 Svn., spinosus Rogers, 1858; Geol. Pennsylvania, vol. 2, p. 816, fig. o90. 
 
 harlani Ordway, 1861 ; Proc. Boston Soc. Nat. Hist., vol. 8, p. 1, figure. 
 
 harlani Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 45, pi. 7, fig. 3, pi. 
 
 8, figs. 1> 1 a-c; pi. 9, fig. 1? 
 
VUGDKS.J 
 
 CATALOGUE OF TRILOBITES. 
 
 131 
 
 Paradoxides kjerulfi (Linrs.) Matthew, 1886 ; Am. Jour. Sci., 3d series, vol. 31, p. 
 471. Cambrian. 
 
 Referred by Holm (Geol. Foren. Stockholm Forhandl., vol. 9, 1887, hafte. 7, 
 p. 1) to Olenellus kjerulfi Linnarsson, pis. 14 and 15. 
 
 lamellatus Hartt, 1868; Acadian Geology, p. 656, fig. 230. .St. John. 
 
 lamellatus Matthew, 1882 ; Trans. Royal Soc. Canada, vol. 1, p. 100, pi. 1, figs. 
 
 3,4. 1 
 
 lamellatus var. loricatus Matthew, 1882; Trans. Royal Soc. Canada, vol. 1, p. 
 
 105, pi. 9, fig. 19. 
 
 lamellatus Walcott, 1884; Bull. U. S. Geol. Survey, No. 30, p. 25, pi. 3, figs. 
 
 2, 2 a. 
 
 macrocephalus. (See Olenellus thompsoni Hall.) 
 
 micmac Hartt, 1868; Acadian Geology, p. 657. St. John. 
 
 micmac Matthew, 1884 ; Trans. Royal Soc. Canada, vol. 2, p. 101, pi. 10, fig. 8. 
 
 ? nevadcnsis. (See Olenoides nevadensis.) 
 
 quadrispinosus. (See Bathynotus quadrispinosus.) 
 
 tenellus Billings, 1874; Pal. Foss., vol. 2, p. 74, fig. 43. Potsdam. 
 
 thompsoni. (See Olenellus thompsoni Hall.) 
 
 triarihrus Harlan ; Trans. Geol. Soc. Pennsylvania, vol. 1, p. 264, pi. 15, fig. 5. 
 
 (See Triarthrus becki Green.) 
 
 vermontana. (See Olenellus and Mesonacis.) 
 
 walcotti Shaler and Foerste, 1888; Bull. Mus. Comp. Zool. Harvard Coll., vol. 
 
 16, p. 36, pi. 2, fig. 12. . Cambrian. 
 
 Peltura Milne-Edwards, 1840; Crust., vol. 3, p. 344. 
 
 (See Pagura.) 
 
 liolopyge. (See Bathynotus holopyge.) 
 
 Pemphigaspis Hall, 1863; 16th Rept. New York State Mus. Nat. Hist., p. 221. 
 
 bullata Hall, 1863 ; 16th Rept. New York State Mus. Nat. Hist., p. 221, pi. 5 a, 
 
 figs. 3-5.* Potsdam. 
 
 A species probably of the genus Microdiscus. 
 
 Phacops Emmrich, 1839; De Trilobites, etc., p. 18. 
 
 Type, Calymene latifrons Broun. 
 
 The generic term Trimerocephalus McCoy has been used by authors for species 
 like Phacops volborthi, compact in form ; glabella inflated and expanded in front; 
 lobes, except the basal ones, obscure; eyes small and occupying the front por- 
 tions of the head ; genal angles rounded ; pleura rounded ; pygidium small, with 
 few segments, and even border. 
 
 Acaste Goldfuss for such species as Phacops downingice Mufch. Diagnosis: 
 Glabella not inflated nor greatly expanded in front ; furrows distinct ; eyes 
 well developed, with numerous lenses; genal angles produced into spines; 
 pleurm rounded or truncate ; pygidium small generally, with less than eleven 
 segments ; border even, but sometimes mucronate. 
 
 [ Calymene ] bufo Green, 1832; Monthly Am. Jour. Geol., p. 559. 
 
 ICalymeue ] bufo Green, 1832; Mon. Tril. N. A., p. 41, cast 10. 
 
 bufo Hall, 1861 ; Des. New Species Foss., p. 65. 
 
 bufo Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 93. 
 
 bufo Hall, 1876; Ulus. Devonian Foss. Crust., pi. 8, figs. 24,25. 
 
 bufo Hall, 1888; Pal. New York, vol. 7, p. 26, 'pi. 8, figs. 25/26. 
 
 The fossil is said to have been found in a dark grayish limestone in the State 
 of New Jersey. The cast approaches so near Phacops latifrons Broun that it 
 may be the same species. 
 
 bombifrons. (See Phacops cristata.) 
 
 cacapona Hall, 1861 ; Des. New Species Foss., p. 68. Hamilton. 
 
 Syn., Calymene bufo Castelnau, 1843; Syst. Sil. do I’Ainer., p. 21, pi. 2, figs. 1-4. 
 cacapona Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 96. 
 
132 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Phacops cacapona Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 8,' figs. 18-23. 
 
 cacapona Hall, 1888; Pal. New York, vol. 7, p. 27, pi, 8, figs. 19-24. 
 
 callicephala. (See Dalmanites callicephala. ) 
 
 cristata Hall, 1861 ; Des. New Species Foss., p. 67. Upper Helderberg. 
 
 Syn., Phacops homhifrons Hall, 1861 ; Des. New Species Foss., p. 67. 
 
 Phacops cristata Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 95. 
 Phacops cristata Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 6, figs. 1-17. 
 Phacops homhifrons Hall, 1876; Illus. Devonian Foss. Crust., pi. 6, figs. 18-29. 
 - — cristata Hall, 1888; Pal. New York, vol. 7, p. 14, pi. 6, figs., 1-31, 16-29; pi. 
 8 a, figs. 1-4. 
 
 cristata var. pipa Hall, 1888; Pal. New York, vol. 7, p. 18, pi. 8 a, figs. .5-18. 
 
 Upper Helderberg. 
 
 doivningce Murcb. (See Phacops trisulcatus Hall.) 
 
 — — hudsonica Hall, 1859; Pal. New York, vol. 3, p. 355, pi. 73, figs. 26-28. 
 
 Lower Helderberg. 
 
 f laticauda Hall, 1847 ; Pal. New York, vol. 1, p. 248, pi. 64, fig. 6. (See Dalmani- 
 tes micrurus Green.) 
 
 logani Hall, 1859 ; Pal. New York, vol. 3, p. 353, pi. 73, figs. 15-25. 
 
 Lower Helderberg. 
 
 [ Cahjmene~\ macrophthalma Green, 1832; Mon. Tril. N. A., p. 39, cast 9. 
 
 [ Calymene'] nupera Hall, 1843; Geol. New York, 4th Geol. Dist., p. 262, fig. 116. 
 
 Chemung. 
 
 nupera Emmons, 1869 ; Manual Geology, p. 149, fig. 138 (2). 
 
 nupera Hall, 1876; Illus. Devonian Foss. Crust., pi. 8, fig. 26. 
 
 nupera Hall, T888; Pal. New York, vol. 7, p. 27, pi. 8, fig. 27. 
 
 orestes Billings, 1860 ; Canadian Naturalist, vol. 5, p. 65, fig. 10. 
 
 Middle Silurian. 
 
 pulchellus Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 99, pi. 8, figs. 4,20,21. 
 
 Clinton. 
 
 \_Calymene hufo] var. rana Green, 1832; Monthly Am. Jour. Geol., p. 559. 
 
 Hamilton. 
 
 [ Calymene hufo] var. rana Green, 1832; Mon. Tril. N. A., p. 42, casts 11, 12. 
 
 ICalymene hufo] var. rana Hall, 1843; Geol. New York, 4th Geol. Dist., p. 201, 
 
 pi. 14. 
 
 Syn., [ Calymene ] hufo Owens, 1844 ; Geol. Expl. Iowa, Wisconsin, and Illinois, p. 
 74, pi. 12, fig. 1. 
 
 {Calymene] hufo Emmons, 1860 ; Manual Geology, p. 138, wood-cutl24, fig. 6. 
 rana Hal>, 1861 ; Description New Species Fossils, p. 65. 
 
 rana Hall, 1862 ; 15th Rept. New York State Cab. Nat. Hist., p. 93, pi. 10, fig. 12. 
 
 rana Meek and Worthen, 1868 ; Geol. Survey Illinois, vol. 3, p. 447, pi. 11, figs. 
 
 1 a-e. 
 
 rana Nicholson, 1873 ; Pal. Province Ontario, p. 123, figs. 5,6 a. 
 
 rana Hall, 1876; Illus. Devonian Foss. Crust., pi. 6, figs. 14, 15; pi. 7, figs. 1-11 ; 
 
 pi. 8, figs. 11-17. 
 
 rana Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 339, pi. 26, figs. 17-19. 
 
 rana Walcott, 1884 ; Pal. Eureka Dist. Mon. U. S. Geol. Survey, vol. 8, p. 207. 
 
 rana Hall, 1888 ; Pal. New York, vol. 7, p. 19, pi. 7, figs. 1-11 ; pi. 8, figs. 1-18 ; 
 
 pi. 7 a, figs. 21-33. 
 
 rana Clarke, 1888 ; Jour. Morphology, vol. 2, p. 253, pi. 21. 
 
 traganus Billings, 1863 ; Proc. Portland Soc. Nat. Hist., vol. 1, p. 124, pi. 1, figs. 
 
 26, 27. Upper Silurian. 
 
 ? trisulcatus Hall, 1843 ; Geol. New York, 4th Geol. Dist., p. 72, fig. 9. 
 
 Clinton. 
 
 trisulcatus Hall, 1852 ; Pal. New York, vol. 2, p. 300, pi. 66 a, figs. 3 a, b. 
 
VOGDES 1 
 
 CATALOGUE OF TRILOBITES. 
 
 133 
 
 Phaethonides Angelin, 1852 ; Pal. Scand., p. 21. 
 
 arenicolus Hall, 1888 ; Pal. New York, vol. 7, p. 134, pi. 25, figs. 12, 13. 
 
 Upper Helderberg. 
 
 denticulatus (Meek) Hall, 1888 ; Pal. New York, vol. 7, p. 139, pi. 25, tigs. 14, 15. 
 
 For other references, see Proetus [ Phceton~\ denticulatus Meek. 
 
 Steptoe Valley, Nevada, Devonian (?). 
 
 gemmaeus Hall, 1888; Pal. New York, vol. 7, p. 136, pi. 24, figs. 32-36. 
 
 Upper Helderberg. 
 
 immaturus Herrick, 1889; Bull. Denison Univ., vol. 4, p. 59, pi. 1, tigs. 9-15. 
 
 Kinderhook. 
 
 (?) lodiensis (Meek) Herrick, 1889; Bull. Denison Univ., vol. 4, p. 59. 
 
 For other references, see Brachymetopus lodiensis Meek. 
 
 occidentals Herrick, 1889; Bull. Denison Univ., vol. 4, p. 57, pi. 1, figs. 10 a, b. 
 
 Kinderhook. 
 
 sedaliensis (Vogdes) Herrick, 1839; Bull. Denison Univ., vol. 4, p. 57. 
 
 Waverly. 
 
 For other references, see Griffithides ? sedaliensis Vogdes. 
 
 spinosus Herrick, 1889; Bull. Denison Univ., vol. 4, p. 58, pi. 1, figs. 4-5. 
 
 Kinderhook. 
 
 varicella Hall, 1888 ; Pal. New York, vol. 7, p. 135, pi. 24, figs. 29-31. 
 
 Upper Helderberg. 
 
 Phillipsia Portlock, 1843; Kept. Geol. Londonderry, etc., p. 315. 
 
 Type, Phillipsia gemmulifera Phillips. 
 
 Dr. Henry Woodward suggests (Geol. Mag., vol. 10, 1883) the following brief 
 diagnosis of the characters of the genera Phillipsia and Griffithides, which may 
 be found useful in separating the genera : 
 
 
 Phillipsia. 
 
 Griffithides. 
 
 1 
 
 Sides of the glabella nearly parallel 
 
 Glabella pyriform. 
 
 2 
 
 Marked by either two or three short lat- 
 eral furrows. 
 
 No short lateral furrows on the glabella. 
 
 3 
 
 Basal lobes continuous with the glabella.. 
 
 Basal lobes distinct from the glabella. 
 
 4 
 
 Eyes large, reniform 
 
 Eyes small, suboval. 
 
 bufo. (See Griffithides bufo.) 
 
 cliftonensis Shumard, 1858 ; Trans. Acad. Nat. Sci. St. Louis, vol. 1, p. 227. 
 
 Coal Measures. 
 
 cliftonensis Herrick, 1887 ; Bull. Denison Univ., vol. 2, p. 11. 
 
 cliftonensis Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4,p. 84. 
 
 ? consors Herrick, 1889 ; Bull. Denison Univ., vol. 4, p. 53, pi. 1, figs. 16 a, b, c. 
 
 Keokuk or Burlington. 
 
 consors Herrick, 1890 ; American Geologist, vol. 5, p. 254. 
 
 f coronata. (See Cyphaspis coronata Hall.) 
 
 dori8 (Hall) Winchell, 1865; Proc. Acad. Nat. Sci. Phila., 2d series, vol. 9, p. 
 
 133. (See Proteus doris Hall.) 
 
 howi Billings, 1863 ; Canadian Naturalist, vol. 8, p. 209, figure. Carboniferous. 
 
 howi Dawson, 1868; Acadian Geology, p. 313, fig. 133. 
 
 howi Herrick, 1887 ; Bull. Denison Uuiv., vol. 2, p. 63. 
 
 howi Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 91. 
 
 Compare Phillipsia meramecensis. 
 
 insignis Winchell, 1863; Proc. Acad. Nat. Sci. Phila., 2d series, vol. 7, p. 24. 
 
 Burlington. 
 
 insignis Billings, 1863; Canadian Naturalist, vol. 8, p. 209. 
 
 insignia Herrick, 1887; Bull. Denison Univ., vol. 2, p. 63. 
 
134 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Phillipsia insignis Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 87. 
 
 Icevis. (See Cyphaspis laevis.) 
 
 major Shumard, 1858; Trans. Acad. Sci. St. Louis, vol. 1, p. 226. Coal Measures. 
 
 major Meek, 1872; U. S. Geol. Survey Territories, Final Rept. Nebraska, p. 238, 
 
 pi. 3, figs. 2 a, b, c. 
 
 major Herrick, 1887 ; Bull. Denison Univ., vol. 2, p. 60. 
 
 major Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 85, pi. 3, fig. 14. 
 
 meramecansis Sbumard, 1855; 1st and 2d Rept. Geol. Survey Missouri, p. 199, 
 
 pi. B, fig. 9. Archimides Limestone. 
 
 meramecansis Herrick, 1887 ; Bull. Denison Univ., vol. 2,p. 59. 
 
 meramecansis Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 86, pi. 3, 
 
 fig. 15. 
 
 Syn., meramecansis ? Winchell, 1863 ; Proc. Acad. Nat. Sci. Phila., 2d series, vol. 7, 
 p. 24. Keokuk. 
 
 meramecansis Herrick, 1888; Bull. Denison Univ., vol. 3, p. 28, pi. 11, fig. 3. 
 
 Syn., howi (Billings) Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 92. 
 
 vindobonensis (Hartt) Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, 
 p. 92. 
 
 meramecansis Herrick, 1889 ; Bull. Denison Univ., vol. 4, p. 54, pi. 1, fig. 6. 
 
 minuscula Hall. (See Cyphaspis minuscula.) 
 
 missouriensis Shumard, 1858 ; Trans. Acad. Sci. St. Louis, vol. 1, p. 220. 
 
 Coal Measures. 
 
 missouriensis Herrick, 1887 ; Bull. Denison Univ., vol. 2, p. 59. 
 
 missouriensis Vogdes, 1887; Annals New York Acad. Sci., vol. 4, p. 86, pi. 3, 
 
 figs. 1, 2, 14, 1& 
 
 ? ornahis. (See Cyphaspis coronata.) 
 
 [ Griffithides j Meek and Worthen. (See Griffithides portlocki.) 
 
 perannulata Shumard, 1858; Trans. Acad. Sci. St. Louis, vol. 1, p. 296, p). 11, 
 
 fig. 10. Permian. 
 
 • perannulata Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 84. 
 
 praecursor Herrick, 1888; Bull. Denison Univ., vol. 3, p. 29, pi. 12, fig. 1. 
 
 Kinderhook. 
 
 praecursor Herrick, 1890 ; American Geologist, vol. 5, p. 254. 
 
 [ Proetus ] praecursor Herrick, 1889; Bull. Denison Univ., vol. 4, p. 54, pi. 1, 
 
 fig. 1. Waverly. 
 
 rockfordensis Winchell, 1865; Proc. Acad. Nat. Sci. Phila., 2d series, vol. 9, p. 
 
 133. Kinderhook. 
 
 rockfordensis Herrick, 1887 ; Bull. Deuison Univ., vol. 2, p. 62. 
 
 rockfordensis Vogdes, 1887; Annals New York Acad. Sci., vol. 4, p. 91. 
 
 sampsoni Vogdes, 1888; Trans. New York Acad. Sci., vol. 7, p. 248, figure. 
 
 Waverly.. 
 
 [ Griffithides ] sangamonensis Meek anu Worthen. (See Griffithides sangamo- 
 
 nensis. ) 
 
 [ Griffithides'] scitula Meek and Worthen. (See Griffithides scitula.) 
 
 - — serraticaudata Herrick, 1889; Bull. Denison Univ., vol. 4, p. 52, pi. 1, figs. 8 
 a-d. Keokuk. 
 
 serraticaudata Herrick, 1890; American Geologist, vol. 5, p. 254. 
 
 shumardi. (See Proetus auriculata.) 
 
 stevensoni Meek, 1871 ; Rept. Regents Univ. West Virginia, p. 73. Chester. 
 
 stevensoni Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 88, pi. 3, fig. 6. 
 
 tuberculata Meek and Worthen, 1870; Proc. Acad. Nat. Sci. Phila., p. 52. 
 
 Burlington. 
 
 tuberculata Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 92. 
 
 trinucleata Herrick, 1887 ; Bull. Denison Univ., vol. 2, p. 64, pi. 1, figs. 23, 23 a, 
 
 c, e, h; pi. 2, fig. 32; pi. 3, fig. 21. Coal Measures. 
 
V0GOER.] 
 
 CATALOGUE OF TRILOBITES. 
 
 135 
 
 Phillipsia trinucleata Herrick, 1889; Bull. Denison Univ., vol. 4, p. 49. 
 
 Syn., Proetus trinucleatus Vogdes, 1888; Annals New York Acad. Sci., vol. 4, p. 
 (in error), pi. 2, figs. 7,8,9. 
 
 vindobonensis Hartt, 1868; Acadian Geology, p. 353. Carboniferous. 
 
 vindobonensis Herrick, 1887; Bull. Denison Univ., vol. 2, p. 63. 
 
 vindobonensis Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 89. (See 
 
 Phillipsia meramecansis Sbumard.) 
 
 Piliolites Cozzens, 1846; Annals Lyceum Nat. Hist. New York, vol. 4, p. 157. 
 
 oliioensis Cozzens, 1846; Annals Lyceum Nat. Hist. New York, vol. 4, p. 157, 
 
 pi. 16, figs. 1 a, 1 b. (See Proetus crassimarginatus ?) 
 
 Proetus Steininger, 1831 ; M6m. Soc. G6ol. France, vol. 1, p. 355, pi. 24, fig. 6. 
 
 Type, Proetus cuvieri Steininger. 
 
 Syn., PEonia Burmeister, 1843; Organization Trilobites, p. 116 (Ray Soci ed., p. 
 
 100). Burmeister separates Dalman’s species Calymene concinna from the 
 type of the genus Proetus , and gives a generic description of JEonia, with 
 descriptions and figures of A. concinna , A. stolcesii, and A. verticalis. 
 
 Phceton Barrande, 1846; Notice Prelim., p. 62. The author hereiu gives the 
 new generic term Phceton for species of Proetus with fimbriated pygidia. 
 
 Prinopeltis Corda, 1847 ; Prodr., p. 121. New generic name proposed for 
 the preoccupied term of Phceton. 
 
 Xiphogonium Corda, 1847 ; Prodr., p. 70. Proposed genus for certain species 
 of Proetus, with nine segments in the thorax. 
 
 Goniopleura. Corda, 1847; Prodr., p. 80. This genus includes such species 
 as Proetus elegantulus Loven, with twelve segments in the thorax. 
 
 Forbesia McCoy, 1847 ; Sil. Foss. Ireland, p. 46. This author uses for the 
 types of his genus Forbesia latifrons and F. stolcesii, which is the same as 
 that used by Barrande in 1846 for his genus Phceton and Angelin in 1878 
 for the genus Phcethonides. 
 
 Gerastos Goldfuss, 1843 ; Neues Jahrbucli fii.r Mineral., p. 557. This genus 
 is a Proetus with G. Icevigatus for its type, a species identical with Proetus 
 cuvieri Stein. 
 
 Trigonaspis and Cylindraspis the Brothers Sanderberger ; Verst, d. Rhein, 
 Scht.-Syst., p. 30, pi. 3, 1850. 
 
 Dechenella Kayser, 1880; Zeitschr. Deutsch. geol. Gesell., Berlin, 1880, p. 
 703. For such species as Proetus verticallis and P. halclemani. 
 
 alaricus Billings, 1860; Canadian Naturalist, vol. 5, p. 68, fig. 12. Hudson. 
 
 alaricus Billings, 1863; Geol. Canada, p. 219, fig. 230. 
 
 angustifrons Hall, 1861 ; Des. New Species Foss., p. 70. Schoharie. 
 
 angustifrons Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 98. 
 
 angustifrons Hall, 1876; Illus. Devonian Foss. Crust., pi. 20, figs. 1,4,7. 
 
 angustifrons Hall, 1888; Pal. New York, vol. 7, n. 91, pi. 20, figs. 1-5; pi. 22, 
 
 figs. 1-3. 
 
 auriculatis. (See Proetus missouriensis Shumard.) 
 
 canaliculatus Hall, 1861 ; Des. New Species Foss., p. 73. Upper Helderberg. 
 
 canaliculatus Hall, 1862; 15t,h Rept. New York State Cab. Nat. Hist., p. 101. 
 
 canaliculatus Hall, 1876; Illus. Devonian Foss. Crust., pi. 20, figs. 10,11. 
 
 canaliculatus Hall, 1888; Pal. New York, vol. 7, p. 107, pi. 20, figs. 10, 11; pi. 
 
 23, figs. 10, 11. 
 
 clarus Hall, 1861 ; Des. New Species Foss., p. 71. Upper Helderberg. 
 
 * clarus Hall, 1862; 15th Rept. New York State Mus. Nat. Hist., p. 99. 
 
 clarus Hall, 1876; Illus. Devonian Foss. Crust., pi. 20, figs. 12-14. 
 
 clarus Hall, 1888 ; Pal. New York, vol. 7, p. 104, pi. 20, figs. 12-14 ; pi. 22, figs. 
 
 28-30. 
 
 conradi Hall, 1861 ; Des. New Species Foss., p. 09. 
 
 Schoharie. 
 
136 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63 . 
 
 Pioetus conradi Hal], 1862; 15tli Rept. New York State Cab. Nat. Hist., p. 97. 
 
 conradi Hall, 1876; Illus. Devonian Foss. Crust., pi. 21, fig. 6 (not figs. 5, 8, 9); 
 
 pi. 21, figs. 27, 28. 
 
 Syn., Conradi Hall, 1876; Illus. Devonian Foss. Crust., pi. 2p, figs. 5,8,9. 
 
 Piliolites ohionensis? Cozzens, 1846; Annals Lyceum Nat. Hist. New York, 
 vol. 7, p. 99, pi. 10, figs. 1 a, b. 
 
 conradi Hall and Clarke, 1888 ; Pal. New York, vol. 7, p. 89, pi. 20, fig. 9 ; nl. 
 
 21, figs. 27,28; pi. 12, fig. 4. 
 
 \_Asaphus'] corycceus Conrad, 1842; Jour. Acad. Nat. Sci. Phila., vol. 8, p. 277, 
 
 pi. 16, fig. 15. Niagara. 
 
 [ Asaphus ] corycceus Hall, 1843 ; Geol. New York, 4th Geol Dist, pi. 19, fig. 3. 
 
 corycceus Hall, 1852; Pal. New York, vol. 2, p. 315, pi. 67, fig. 15. 
 
 [ Calymene ] crassimarginatus Hall, 1843; Geol. New York, 4th Geol. Dist., p. 
 
 172, fig. 5. Upper Helderberg. 
 
 crassimarginatus Hall, 1859 ; 12th Rept. New York State Cab. Nat. Hist., p. 88. 
 
 [ Pkillipsia ] crassimarginatus Billings, 1861 ; Canadian Journal, vol. vi, p. 362. 
 
 crassimarginatus Hall, 1861 ; Des. New Species Foss., p. 72. 
 
 crassimarginatus Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 
 
 100, pi. 10, fig. 10. 
 
 crassimarginatus Hall, 1876; Illus. Devonian Foss. Crust., pi. 20, figs. 20-31. 
 
 crassimarginatus Hall, 1888; Pal. New York, vol. 7, p. 99, pi. 20, figs. 6-8, 20- 
 
 31; pi. 22, figs. 20-62; pi. 25, fig. 8. 
 
 curvimarginatus Hall, 1888 ; Pal. New York, vol. 7, p. 94, pi. 22, figs. 13-19. 
 
 Schoharie. 
 
 davenportensis Harris. (See Froetus prouti Shumard.) 
 
 dephinulus Hail, 1888; Pal. New York, vol. 7, p. Ill, pi. 23, figs. 1, 2; pi. 25, 
 
 fig. 6. Upper Helderberg. 
 
 denticulatus Meek, 1877; U. S. Geol. Expl. 40th Par., vol. 4, p. 49, pi. 1, figs. 
 
 10 a, b. Devonian. 
 
 determinatus Foerste, 1887 ; Bull. Denison Univ., vol. 2, p. 91, pi. 8, figs. 2, 3, 3 a. 
 
 Clinton. 
 
 doris Hall, 1860; 13th Rept. New York State Cab. Nat. Hist., p. 112. 
 
 Goniatite limestone. 
 
 [ Pkillipsia ] doris Winchell, 1865 ; Proc. Acad. Nat. Sci. Phila., 2d series, vol. 2, 
 
 p. 62. 
 
 [Pkillipsia'] doris Herrick, 1887 ; Bull. Denison Univ., vol. 2, p. 62. 
 
 [ Pkillipsia ] doris Vogdes, 1887; Annals New York Acad. Sci., vol. 4, p. 90 (in 
 
 error). 
 
 ellipticus Meek and Worthen, 1865 ; Proc. Acad. Nat. Sci. Phila., p. 267. 
 
 Kinderhook. 
 
 ellipticus Meek and Worthen, 1868; Geol. Survey Illinois, vol. 3, p. 460, pi. 14, 
 
 fig. 3. 
 
 ellipticus Yogdes, 1887; AnDals New York Acad. Sci., vol. 4, p. 82, pi. 3, fig. 3. 
 
 folliceps Hall, 1888 ; Pal. New York, vol. 7, p. 101, pi. 23, figs. 3-8. 
 
 Upper Helderberg. 
 
 granulatus Wetherby. (See Griffithides granulatus.) 
 
 haldemani Hall, 1861; Des. New Species Foss., p. 74. Hamilton. 
 
 haldemani Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 102, pi. 
 
 10, fig. 6. 
 
 haldemani Hall, 1876; Illus. Devonian Foss. Crust., pi. 21, figs. 7-9. 
 
 haldemani Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 210. 
 
 haldemani Herrick, 1889 ; Bull. Denison Univ., vol. 4, p. 55, pi. 1, fig. 12. 
 
 haldemani Hall, 1888 ; Pal. New York, vol. 7, p. 113, pi. 21, figs. 7-9; pi. 23, figs. 
 
 13 - 15 . 
 
vogdes.] CATALOGUE OF TRILOBITES. 137 
 
 Proetus [Dechenella] haldemani Kayser, 1880; Zeitscbr. Deutsch. geol. Gesell., Ber- 
 liu, 1880, p. 770, pi. 27, fig. 9. 
 
 [ Dechenella ] haldemani Tscliernyschew, 1887 ; M6m. Comity G6ol., vol. 3, No. 3, 
 
 p. 14, pi. 1, fig. 9. 
 
 hesione Hall, 1861 ; Des. New Species Foss., p. 70. Schoharie. 
 
 hesione Hall, 1862; 15th Kept. New York State Cab. Nat. Hist., p. 98. 
 
 - — hesione Hall, 1876; Illus. Devonian Foss. Crust., pi. 20, figs. 15, 16. 
 
 hesione Hall, 1888; Pal. New York, vol. 7, p. 93, pi. 20, figs. 15, 16. 
 
 jejunus.Hall, 1888; Pal. New York, vol. 7, p. 124, pi. 25, fig. 7. Hamilton. 
 
 — — junius Billings, 1863 ; Proe. Portland Soc. Nat. Hist., vol. 1, p. 122, pi. 1, fig. 23. 
 
 Upper Silurian. 
 
 latimarginatus Hall, 1888; Pal. New York, vol. 7, p. 97, pi. 22, figs. 7-12. 
 
 Schoharie. 
 
 loganensis Hall and Whitfield, 1877; U. S. Geol. Expl., 40th Par., vol. 4, p. 
 
 264, pi. 4, fig. 33. Waverly. 
 
 loganensis Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 78. 
 
 longicaudus Hall, 1861 ; Des. New Species Foss., p. 80. Hamilton. 
 
 longicaudus Hall, 1862; 15th Kept. New York State Cab. Nat. Hist., p. 108, 
 
 pi. 10, figs. 7-9. 
 
 longicaudus Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 20, figs. 32-34. 
 
 longicaudus Williams, 1881 ; Am. Jour Sci., 3d series, vol. 21, p. 156. 
 
 (?) longicaudus Hall, 1888; Pal. New York, vol. 7, p. 131, pi. 20. figs. 32-34. 
 
 macrobius Billings, 1863; Proc. Portland Soc. Nat. Hist., vol. 1, p. 123, pi. 1, 
 
 fig. 24. Upper Silurian. 
 
 macrocephalus Hall, 1861 ; Des. New Species Foss., pp. 77, 79. Hamilton. 
 
 macrocephalus Hall, 1862; 15th Kept. New York State Cab. Nat. Hist., pp. 
 
 105, 107. 
 
 macrocephalus Hall, 1876 ; Illus. Devonian Foss. Crust., pi. 21, figs. 10-21. 
 
 macrocephalus Hall, 1888; Pal. New York, vol. 7, p. 116, pi. 21, figs. 10-21 ; pi. 
 
 23, fig. 30. 
 
 [Calymene] marginalis Conrad, 1839; Ann. Rept. Pal. Dept. New York Geol. 
 
 Survey, p. 66. Tully Limestone. 
 
 marginalis Hall, 1861 ; Des. New Species Foss., p. 76. Hamilton. 
 
 marginalis Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 104. 
 
 marginalis Hall, 1876; Illus. Devonian Foss. Crust., pi. 21, figs. 24-28. 
 
 marginalis Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 210. 
 
 marginalis Hall, 1888 ; Pal. New York, vol. 7, p. 122. 
 
 • microgemma Hall, 1888 ; Pal. New York, vol. 7, p. 109, pi. 22, figs. 33, 34. 
 
 Upper Helderberg. 
 
 minuscula Hall, 1876; Illus. Devonian Foss. Crust., pi. 20, fig. 17. 
 
 minutus Herrick, 1889; Bull. Denison Univ., vol. 4, p. 56, pi. l,figs. 7 a, b. 
 
 Kinderliook. 
 
 minutus Herrick, 1890 ; American Geologist, vol. 5, p. 254. 
 
 missouriensis Shumard, 1855; 1st and 2d Rept. Geol. Missouri, p. 196, pi. B, 
 
 figs. 13 a, b. Waverly. 
 
 Syn., auriculatus Hall, 1861 ; Des. New Species Foss., p. 79. 
 
 auriculatus Hall, 1862; 15th Rept. New York State Cab. Nat. Ilist., p. 107. 
 [ Phillipsia (Proetus)] auriculatus Herrick, 1889; Bull. Denison Univ., vol. 
 4, p. 34, pi. 1, fig. 14. 
 
 [ Phillipsia ] shumardi Herrick, 1887 ; Bull. Denison Univ., vol. 2, pp. 58, 69, 
 pi. 7, fig. 14. 
 
 missouriensis Vogdes, 1887; Annals Now York Acad. Sci., vol. 4, p. 75, pi. 3, 
 
 tig. 1. 
 
 missouriensis Hall, 1888; Pal. New York, vol. 7, p. 133, pi. 23, fig. 32. 
 
138 • A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [BULL. 63. 
 
 Proetus occidens Hall, 1861 ; Des. New Species Foss., p. 80. Hamilton. 
 
 occidens Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 108. 
 
 occidens Hall, 1876; Illus. Devonian Foss. Crust., pi. 21, figs. 22,23. 
 
 occidens Hall. 1888; Pal. New York, vol. 7, p. 130, pi. 21, figs. 22,23. 
 
 ovifrons Hall, 16 b 8; Pal. New York, vol. 7, p. 110, pi. 22, figs. 31, 32. 
 
 Upper Helderberg. 
 
 — — pachydermatus Barrett, 1873; Am. Jour. Sci., 3d series, vol. 15, p. 370. 
 
 Niagara. 
 
 — — parviusculus Hall, 1872 ; 24th Rept. New York State Cab. Nat. Hist., p. 223, pi. 
 8, fig. 14. Hudson. 
 
 parviusculus Hall and Whitfield, 1875; Pal. Ohio, vol. 2, p. 109, pi. 4, fig. 18. 
 
 parviusculus Miller, 1874; Cincinnati Quart. Jour. Sci., vol. 1, p. 144. 
 
 - — peroccidens Hall and Whitfield, 1877 ; U. S. Geol. Expl. 40th Par. , Pal. , vol. 4, 
 p. 262, pi. 4, figs. 28-32. Waverly. 
 
 peroccidens Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 79. 
 
 phocion Billings, 1874; Pal. Foss., vol. 2, p. 63, fig. 31. Devonian. 
 
 phocion Hall, 1888; Pal. New York, vol. 7, p. 125, pi. 25,. figs. 9,10. 
 
 planimarginatus Meek, 1871 ; Proc. Acad. Nat. Sci. Pliila., p. 89. Corniferous. 
 
 planimarginatus Meek, 1873 ; Pal. Ohio, vol. 1, p. 233, pi. 23, figs. 3 a, b. 
 
 planimarginatus Hall, 1888; Pal. New York, vol. 7, p. 112, pi. 23, fig. 12. 
 
 protuberans Hall, 1859; Pal. New York, vol. 3, p. 351, pi. 73, figs. 5-8. 
 
 Lower Helderberg. 
 
 — — prouti Shumard, 1863; Trans. Acad. Sci. St. Louis, vol. 2, p. 110. Hamilton. 
 Syn., davenportensis Barris, 1878; Proc. Davenport Acad. Sci., vol. 2, p. 287, pi. 
 11, fig. 8. (pi. 11, fig. 8, revised). 
 
 prouti Hall, 1888; Pal. New York, vol. 7, p. 126, pi. 23, figs. 16-18. 
 
 [ Calymene~\ rowi Le Row, 1837 ; Poughkeepsie Telegram, Nov. 22. Hamilton. 
 
 [ Calymeno ] rowi Green, 1838; Am. Jour. Sci., 1st series, vol. 33, p. 406. 
 
 ■ [ Calymene ] rowi Green, 1838; AnnalsMag. Nat. Hist., 1st series, London, vol. 1, 
 
 p. 79. 
 
 rowi Hall, 1861 ; Des. New Species Foss., p. 75. 
 
 rowi Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 103. 
 
 rowi Hall, 1876; Illus. Devonian Foss. Crust., pi. 21, figs. 2-6. 
 
 rowi Hall, 1888; Pal. New York, vol. 7, p. 119, pi. 21, figs. 2-6, 24-26; pi. 23, 
 
 figs. 20-29. 
 
 [ Phillipsia ] shumardi Herrick, 1887; Bull. Denison Univ., vol. 2, pp. 58,69, pi. 
 
 7, figs. 14 a, b. Waverly. 
 
 [ Phillipsia ] shumardi Herrick, 1888; Bull. Denison Univ., vol. 3, p. 29. 
 
 spurlocki Meek, 1872; Am. Jour. Sci., 3d series, vol. 3, p. 426. Hamilton. 
 
 spurlocki Meek, 1873; Pal. Ohio, vol. 1, p. 161, pi. 14, fig. 12. 
 
 spurlocki Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 145. 
 
 stenopyge Hall, 1888 ; Pal. New York, vol. 7, p. 110, pi. 22, fig. 27. 
 
 Upper Helderberg. 
 
 stokesi (Mureh.) Hall, 1852; Pal. New York, vol. 2, p. 316, pi. 67, figs. 13, 14. 
 
 Niagara. 
 
 swallowi Shumard, 1855; 1st and 2d Rept. Geol. Survey Missouri, p. 196, pi. B, 
 
 figs. 12 a, b. Waverly. 
 
 [ Phillipsia ] swallowi Herrick, 1887 ; Bull. Denison Univ., vol. 2, p. 58. 
 
 [ Phillipsia ] tennesseensis Winchell, 1869; Geol. Tennessee, p. 445. Waverly. 
 
 tennesseensis Vogdes, 1887 ; Annals New York Acad. Sci., vol. 4, p. 80. ‘ 
 
 tumidus Hall, 1888; Pal. New York, vol. 7, p. 113, pi. 23, fig. 9. 
 
 Upper Helderberg. 
 
 verneuilli Hall, 1861 ; Des. Now Species Foss., p. 73. Upper Helderberg. 
 
 verneuilli Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 101. 
 
 verneuilli Hall, 1876; Illus. Devonian Foss. Crust., p. 20, figs. 18, 19. 
 
139 
 
 vogdes. j CATALOGUE OF TKILOBITES. 
 
 Proetus verneuilli Hall, 1888; Pal. New York, vol. 7, p. 108, pi. 20, figs. 18, 19. 
 Protichnites Owen, 1852; Quart. Jour. Geol. Soc. London, vol. 8, p. 214. 
 
 alternans Owen, 1852; Quart. Jour. Geol. Soc. London, vol. 8, p. 221, pi. 8 a, 
 
 7. Potsdam. 
 
 carbonarius Dawson, 1873; Am. Jour. Sci., 3d series, vol. 5. Coal Measures. 
 
 latus Owen, 1852; Quart. Jour. Geol. Soc. London, vol. 8, p. 218, pi. 11. 
 
 Potsdam. 
 
 - — lineatus Owen, 1852; Quart. Jour. Geol. Soc. London, vol. 8, p. 220, pi. 8 a, 
 Pi* Potsdam. 
 
 logananus Marsh, 1869; Am. Jour. Sci., 2d series, vol. 48, p. 46. Potsdam. 
 
 multinotatus Owen, 1852; Quart. Jour. Geol. Soc. London, vol. 8, p. 219, pi. 12. 
 
 Potsdam. 
 
 octo-notatus Owen, 1852; Quart. Jour. Geol. Soc. London, vol. 8, p. 217, pi. 10. 
 
 Potsdam. 
 
 septem-notatus Owen, 1852 ; Quart. Jour. Geol. Soc. London, vol. 8, p. 214, pi. 9. 
 
 Potsdam. 
 
 Protypus Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 211. 
 
 [ Angelina ] hitchcocki Whitfield, 1884; Bull. Am. Mus. Nat. Hist., New York, 
 
 vol. 1, p. 148, pi. 14, fig. 13. Potsdam. 
 
 hitchcocki Walcott 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 211, pi. 31, fig. 4. 
 
 [Bathy unis'] senectus Billings, 1861 ; Geol. Vermont, vol. 2, p. 953, figs. 359, 360. 
 
 Middle Cambrian. 
 
 [Bathyurus] senectus Billings, 1861; Pamphlet published in adv. Pal. Foss. 
 
 Canada, p. 15, figs. 20, 21. 
 
 [ Bathijurus ] senectus Billings, 1863; Geol. Canada, p. 286, figs. 298 a,b. 
 
 [ Bathijurus ] senectus Billings, 1865; Pal. Foss., vol. 1, p. 15, figs. 20,21. 
 
 senectus Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 213, pi. 31, figs. 2, 
 
 2 a-c. 
 
 Pterocephalia Roemer, 1852 ; Kreid. von Texas, p. 93. 
 
 [Conocephalites (Pterocephalia)} laticeps Hall and Whitfield. 1877; U. S. Geol. 
 
 Expl. 40th Par., vol. 4, p. 221, pi. 2, figs. 4-7. Potsdam. 
 
 IPtyclioparia ( Pterocephalia )] laticeps Walcott, 1884; Pal. Eureka Dist., Mon. 
 
 U. S. Geol. Survey, vol. 8, p. 69. 
 
 IPtyclioparia (Ptwocephalia)'] occidens Walcott, 1884; Pal. Eureka Dist., Mon. 
 
 U. S. Geol. Survey, vol. 8, p. 58, pi. 9, fig. 21. Cambrian. 
 
 sancti-sabae Roemer, 1849; Texas, p. 421. Potsdam. 
 
 sancti-sabae Roemer, 1852; Kreid. von Texas, p. 93, pi. 11. 
 
 Ptychaspis Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 170. 
 
 Type, Ptychaspis miniscaensis Hall. 
 
 barabuensis Winchell, 1864; Am. Jour. Sci., 2d series, vol. 37, p. 230. Potsdam. 
 
 [ Arionellus ] cylindricus Billings, 1865; Pal. Foss., vol. 1, p. 406, fig. 385. 
 
 IConoceph. ( Ptychaspis ?)] explanatus Whitfield, 1880; Ann. Rept. Geol. Survey 
 
 Wisconsin, 1879, p. 48. Potsdam. 
 
 \_Conoceph. ( Ptychaspis ?)] explanatus Whitfield, 1882; Geol. Wisconsin, vol. 4, 
 
 p. 181, pi. 1, figs. 27, 28. 
 
 Syn granulosa Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 173 
 pi. 6, figs. 33-4 ). 
 
 granulosa Whitfield, 1878; Ann. Rept. Geol. Survey Wisconsin, 1877, p. 34. 
 granulosa Whitfield, 18-42; Geol. Wisconsin, vol. 4, p. 185, pi. 1, fig. 24. 
 
 In this work Ptychaspis granulosa Hall (not Owen) is referred to Ptychaspis 
 striata. 
 
 granulosa Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 185, pi. 1, fig. 24. 
 
 Syn., Dikeloccphalus miniscaensis Owen, 1852; Rept. Geol. Survey Wisconsin, 
 Iowa, and Minnesota, p. 574, pi. 1, figs. 3, 12 ; pi. I a, figs. 4. 5. 
 
 iDikelocephalus-) granulosus Owen, 1852;* Rept. Geol. Survey Wisconsin, Iowa 
 
 and Minnesota, p. 575, pi. 1, fig. 7. Potsdam. 
 
[bull. G3. 
 
 140 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Ptychaspis miniscaensis Hall, 1863; lGfcli Kept. New York State Cab. Nat. Hist., p. 
 171, pi. 6, figs. 41-46; pi. 10, figs. 21 , 22. 
 
 minuta Whitfield, 1878; Aun. Kept. Geol. Survey Wisconsin, 1877, p. 55. 
 
 Potsdam. 
 
 minuta Whitfield, 1882 ; Geol. Wisconsin, vol. 4, p. 186, pi. 1, figs. 25, 26. 
 
 minuta Walcott, 1884 ; Pal. Eureka Dist., Mon. U. Geol. Survey, vol. 8, p. 60, pi. 
 
 10, fig. 23. 
 
 pustulosa Hall and Whitfield, 1877; U. S. Geol. Expl. 40th Par., Pakeont., vol. 
 
 4, p. 223, pi. 2, fig. 27. Potsdam. 
 
 [lHkeloceplialus ] sesostris Billings, 1865; Pal. Foss., vol. 1, p. 198, fig. 184. 
 
 Quebec. 
 
 speciosus Walcott, 1879; 32d Rept. New York State Mus. Nat. Hist., p. 131. 
 
 Calciferous. 
 
 striata Whitfield, 1878; Ann. Rept. Geol. Survey Wisconsin, 1877, p. 55. * 
 
 Potsdam. 
 
 striata Whitfield, 1880; Ann. Rept. Geol. Survey Wisconsin, 1879, p. 51. 
 
 striata Whitfield, 1882 ; Geol. Wisconsin, vol. 4, p. 186. 
 
 Syn., granulosa Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 173, 
 pi. 6, figs. 33-40. 
 
 [ Arionellus] subclavatus Billiugs, 1860; Canadian Naturalist, vol. 5, p. 315, 
 
 figs. 15, 15 a. Quebec. 
 
 Ptychoparia Corda, 1847 ; Prodr., p. 141, pi. 2, fig. 11. 
 
 Type, Ptychoparia striatus Emmrich. 
 
 [ Conocephalites ] adamsi Billings, 1861 ; Pamphlet published in adv. Pal. Foss., 
 
 p. 12, figure. * 
 
 [ Conoceplialus'] Adams, 1848; Am. Jour. Sci., 2d series, vol. 5, p. 109. 
 
 [ Conocephalites ] adamsi Billings, 1861 ; Geol. Vermont, vol. 2, p. 950, fig. 355.- 
 
 [ Conoceplialus ] Billings, 1861; Am. Jour Sci., 2d series, vol. 32, p. 231. 
 
 [ Conoceplialus ] Billings, 1861; Canadian Naturalist, vol. 6, p. 324. 
 
 [ Conocephalites ] adamsi Billings, 1863; Geol. Canada, p. 286, lig. 294. 
 
 [Conocephalites] adamsi Billings, 1865; Pal. Foss., vol. 1, p. 12, fig. 15. 
 
 adamsi Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 195, pi. 26, figs. 1, 
 
 1 a-c. Middle Cambrian. 
 
 Syn., arenosus (Billings) Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 195. 
 
 [ Eulomaf ] aflinis Walcott, 1882; Pal. Eureka Dist., Mon. U. S. Geol. Survey, 
 
 vol. 8, p. 54, pi. 10, fig. 12. Cambrian and Silurian. 
 
 [Crepicephalus (Bath yarns)] angulatus Hall and Whitfield, 1877; U. S. Geol. 
 
 Expl. 40th Par., Palseont., vol. 4, p. 220, pi. 2, fig. 28. Potsdam. 
 
 ? angulatus Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 269. 
 
 ? annectans Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 91, pi. 12, fig. 18. Cambrian. 
 
 [ Crepicephalus (Loganellus)] anytus Hall and Whitfield, 1877; U. S. Geol. Expl. 
 
 40th Par. vol. 4, p. 219, pi. 2, figs. 19-21. Potsdam. 
 
 anytus Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 56, 
 
 pi. 9, fig. 26. 
 
 [ Lisostracus ] anytus Brogger, 1886; Geol. Foren. Stock. Forhandl., vol. 8, p. 212. 
 
 [Conoceph.] antiquatus Salter, 1859; Quart. Jour. Geol. Soc. London, vol. 15, p. 
 
 554, fig. 2. Potsdam. 
 
 Syn., [Conoceph. ~) arenosus Billings, 1861 ; Geol. Vermont, vol. 2, p. 952, fig. 358. 
 
 [ Conoceph. ] arenosus Billings, 1861; Pamphlet published in advance of Pal. 
 
 Foss. Canada, vol. 1 ; also, Pal. Foss., vol. 1, p. 15, fig. 18. 
 
 [Conoceph. J arenosus Billings, 1863; Geol. Canada, p. 286, fig. 297. 
 
 Walcott (Bull. U. S. Geol. Survey, No. 30, p. 195) refers this species to Pty- 
 choparia adamsi. 
 
vogdes. ] CATALOGUE OF TRILOB1TES. 141 
 
 Ptychoparia [ Conoceph . ] aurora Hartt, 1868 ; Acadian Geology, p. 653. (See Ptycho- 
 paria ouangondianus.) 
 
 [ Conoceph .] billingsi Shumard, 1861 ; Am. Jour. Sci., 2d series, vol. 32, p. 219. 
 
 Potsdam. 
 
 [Conoceph. f] binodosus Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., 
 
 p. 16U, pi. 7, fig. 47. Potsdam. 
 
 [Solenopleura f ] breviceps Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. 
 
 Survey, vol. 8, p. 49, pi. 10, fig. 9. Cambrian. 
 
 [Conocephalites] calymenoides Whitfield, 1878; Ann. Rept. Geol. Survey Wis- 
 consin, 1877, p. 52. Potsdam. 
 
 [ Conocephalites ] calymenoides Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 179, 
 
 pi. 3, figs. 2-5. 
 
 calymenoides Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 
 
 8, p. 48. 
 
 [Crepicephalus ( Loganellus )] centralis Whitfield, 1880 ; Geol. Resources Black 
 
 Hills Dakota, p. 341, pi. 2, figs. 21-24. Potsdam. 
 
 [Conocephalites] chippewaensis (Owen) Shumard, 1863; Trans. St. Louis Acad. 
 
 Sci., vol. 2, p. 104. 
 
 [ Lonchocephalus ] chippewaensis Owen, 1852; Rept. Geol. Survey Wisconsin, 
 
 Iowa, and Minnesota, p. 576, pi. 8, figs. 6, 14 ; pi. 1 a, fig. 9. 
 
 ? (subgenus ?) clavata Walcott, 1887 ; Am. Jour. Sci., 3d series, vol. 34, p. 198, 
 
 pi. 1, fig. 3. * Cambrian. 
 
 [ Conoceph ] cordillerae Rominger, 1887 ; Proc. Acad. Nat. Sci. Pliila., p. 17, pi. 1, 
 
 fig. 7. Cambrian. 
 
 cordillerae Walcott, 1888; Am. Jour. Sci., 3d series, vol. 36, p. 165. 
 
 [Conoceph] depressus Shumard, 1861; Am. Jour. Sci., 2d series, vol. 32, p. 219. 
 
 Potsdam. 
 
 [Conoceph] diadematus Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., 
 
 p. 167, pi. 7, figs. 36-39; pi. 9, figs. 18-21 (?). Potsdam. 
 
 [Eulomaf] dissimilis Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, 
 
 vol. 8, p. 51, pi. 9, fig. 28. Cambrian. 
 
 [Conoc&ph (Arionellus ?)] dorsalis Hall, 1863; 16th Rept. New York State Cab. 
 
 Nat. Hist., p. 222. • Potsdam. 
 
 [Conoceph] elegans Hartt, 1868; Acadian Geology, p. 650, St. John. 
 
 [Conoceph] eos Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 151, 
 
 pi. 7, figs. 24, 25; pi. 8, figs. 2-9. Potsdam. 
 
 eos Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 51. 
 
 [ Conoceph. ] eryon Hall, 1863 ; 16th Rept. New York State Cab. Nat. Hist., p. 157, 
 
 pi. 7, figs. 10-16; pi. 8, figs. 16,31. Potsdam. 
 
 fitchi Walcott, 1887; Am. Jour. Sci., 3d sories, vol. 34, p. 197, pi. 1, fig. 6. 
 
 Cambrian. 
 
 [Conoceph.] formosm Hartt. (See Ptychoparia robbi Hartt.) 
 
 [Conoceph. ( Ptychoparia )] gallatinensis Meek, 1873; 6th Ann. Rept. U. S. Geol. 
 
 Survey Territories, 1872,' p. 485. Potsdam. 
 
 Referred by Walcott to Ptychoparia oweni Meek and Hayden. 
 
 [Crepicephalus [Loganellus]) granulosus Hall and Whitfield, 1877; U. S. Geol. 
 
 Expl. 40th Par., Palseont., vol. 4, p. 214, pi. 2, figs. 1, 2, 3. Potsdam. 
 
 granulosus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 57. 
 
 [Crepicephalus (Loganellus)] haguei Hall and Whitfield, 1877; U. S. Geol. Expl. 
 
 40th Par., Pabeont., vol. 4, p. 210, pi. 2, figs. 14, 15. Potsdam. 
 
 haguei Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 57. 
 
 [ Lisostracus ] haguei Brogger, 1886; Geol. Foreningens Stockholm Forhandl., 
 
 vol. 8, p. 202. 
 
 [Conoceph. ] halli Hartt. (Sec Ptychoparia orestes Hartt.) 
 
142 
 
 A BIBLIOGRAPHY OF PALEOZOIC . CRUSTACEA., 
 
 [BULL. 63 . 
 
 Ptychoparia housensis Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 201, pi. 25, 
 fig. 5. Middle Cambrian, 
 
 [Conocoryphe (Concephalites)] kingii Meek, 1870; Proe. Acad. Nat. Sci. Pliila., 
 
 vol. 22, p. 63. 
 
 [Conocoryphe (Concephalites)] kingii Meek, 1877 ; U. S. Geol. Expl. 40th Par., 
 
 Pakeont., vol. 4, p. 20, pi. 1, tig. 4. 
 
 [_ Conocoryphe ( Ptychoparia )] kingii Meek, 1873; 6th Ann. Kept. U. S. Geol. Sur> 
 
 vey Territories, 1872, p, 487. 
 
 [Conocoryphe ( Ptychoparia )] kingii White, 1876; U. S. Geog\ and Geol. Surveys 
 
 West 100th Mer., Palseont., vol. 4, p. 40, pi. 2, tigs. 2 a, b, c. 
 
 [Liostracus] kingii Brogger, 1^86; Geol. Foreningens Stockholm Forhandi., 
 
 vol. 8, p. 205. 
 
 -• - • kingii Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 193, pi. 27, figs. 4, 4 a. 
 
 Middle Cambrian. 
 
 laeviceps Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 54, pi. 10, figs. 17, 18. Cambrian. 
 
 [Conoceplialites (Pterocephalus)] laticeps Hall and Whitfield, 1877; U. S. Geol. 
 
 Expl. 40th Par., Pakeont., vol. 4, p. 67, 221, pi. 2, figs, 4-7. Cambrian. 
 
 — — [ Pterocephalus ] laticeps Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Sur" 
 vey, vol. 8, p. 59. 
 
 ? linnarssoni Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 47, pi. 9, figs. 18, 18 a. • Cambrian. 
 
 [ Loganellus ] logani Devine, 1863; Canadian Naturalist, vol. 8, p. 95, figure. 
 
 Potsdam. 
 
 [ Olenusf ] logani Billings, 1865; Pal. Foss., vol. 1, p. 201, figs. 185, 186. 
 
 Syn., [ Loganellus'] quebecensis Billings ; idem., p. 203. 
 
 logani Walcott, 1884 ; Bull. U S. Geol. Survey, No. 10, p. 36. 
 
 [Crepicephalus {Loganella)] maculosus Hall and Whitfield, 1877; U. S. Geol. 
 
 Expl. 40th Par., Palseont., vol. 4, p. 215, pi. 2, figs. 21, 25, 26(?). Potsdam. 
 
 maculosus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, pj). 
 
 269, 271. 
 
 [ Conoceph. ] minor Shumard, 1863 ; Traus. Acad. Nat. Sci St. Louis, vol. 2, p. 105. 
 
 Potsdam. 
 
 (Undet.) tri lob ite Owen, 1848; Geol Recounoissance Chippewa Land Dist., p. 15, 
 
 pi. 7, fig. 4. 
 
 [Conoceph.] minor Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 149, 
 
 pi. 8, figs. 1-4. 
 
 mijior Walcott, 1884; Pal. Eureka Dist., Mon. U S. Geol Survey, vol. 8, p. 91. 
 
 [Conoceph.] minutus Bradley, 1860; Am. Jour. Sci., 2d series, vol. 30, p. 24, 3 
 
 figs. Potsdam. 
 
 [Conoceph. ] minutus Bradley, 1860; Canadian Naturalist, vol. 5, p. 420, figs. 1-3. 
 
 [ Conoceph. ] minutus Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 
 
 150, pi. 8, figs. 5-7. . 
 
 minutus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 91. 
 
 minutus Walcott, 18feS6; Bull. U. S. Geol. Survey, No. 30, p. 21. 
 
 [Conoceph.] miser Billings, 1861 ; New or little known Sil. Foss., p. 12, fig. 14. 
 
 Potsdam. 
 
 [Conoceph.] miser Billings, 1861 ; Geol. Vermont, vol. 2, p. 950, fig. 354. 
 
 [ Conoceph. ] miser Billings, 1863; Geol. Canada, p. 286, fig. 393. 
 
 [Conoceph.] miser Billings, 1865 ; Pal. Foss., vol. 1, p. 12, fig. 14. 
 
 miser Walcott, 1886; Bull. U. S. Geol Survey, No 30, p. 199, pi. 27, fig. 2. 
 
 [Crepicephalus (Loganella)] montanensis Whitfield, 1876; Rept. Recon Upper 
 
 Missouri, p. 141, pi. 1, tigs. 1, 2. Potsdam. 
 
 montanensis Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 pp. 53, 56, 
 
V0GDB8. ] 
 
 CATALOGUE OF TRILOBITES. 
 
 143 
 
 Ptychoparia mucronatus Shaler and Foerste, 1888 ; Bull. Mus. Comp. Zool. Har- 
 vard Coll., vol. 16, p, 37, pi. 2, fig. 21. Cambrian. 
 
 [Conocepli.] nasutus Hall, 1863; 16tli Kept. New York State Cab. Nat. Hist., p. 
 
 155, pi. 7, figs. 3-9. Potsdam. 
 
 [ Conocepli .] neglectus. (See Ptychoparia tener.) 
 
 — — [Crepiceplialus {Loganella)] nitidus Hall and Whitfield, 1877; U. S. Geol. Expl. 
 40th Par., Palieont., vol. 4, p. 212, pi. 2, figs. 8-10. Cambrian. 
 
 Syn., Crepicephalus [ Loganella J simulator (Hall and Whitfield) Walcott. 
 
 nitidus Walcott, 1884 ; Pal. Eureka Dist., Mou. U. S. Geol. Survey, vol. 8, p. 57. 
 
 — occidentalis Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 p. 51, pi. 10, fig. 5. Cambrian. 
 
 [ Conocepli. ] orestes Hartt, 1868; Acadian Geology, p. 649, fig. 225. St. John. 
 
 Syn., Conocepli . halli (Hartt) Walcott; Bull. U. S. Geol. Survey, No. 10, p. 40. 
 
 Conocepli. thersites (Hartt; Walcott; Bull. U. S. Geol. Survey, No. 10, p. 40. 
 
 orestes var. thersites Walcott, 1884 ; Bull. U. S. Geol. Survey, No. 10, p. 40. 
 
 Syn., orestes Walcott, 1884 ; Bull. U. S. Geol. Survey, No. 10, p. 39, pi. 5, figs. 3, 
 3 a, 
 
 [ Solenopleura] orestes Matthew, 1887 ; Trans. Royal Soc, Canada, vol. 4, p. 154. 
 
 pi. 2, figs. 4 a-e. 
 
 [ Pterocephalus ] occidens Walcott, 1884; Pal. Eureka Dist'., Mon. U. S. Geol. Sur- 
 vey, vol. 8, p. 58, pi. 9, fig. 21. Cambrian. 
 
 [ Conocepli .] ouangondiana Hartt, 1868; Acadian Geology, p. 651, fig. 226. 
 
 St. John. 
 
 ouangondiana Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 37, pi. 5, figs. 
 
 4, 4 a-f. 
 
 ouangondiana var. aurora (Hartt) Walcott; Bull. U. S. Geol. Survey, No. 10, 
 
 p. 38, pi. 5, fig. 5. 
 
 [ Liosiracii8 ] ouangondiana Matthew, 18S7 ; Trans Royal Soc. Canada, p. 138. 
 
 oweni (Meek and Hayden) Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. 
 
 Survey, vol. 8, p. 55, pi. 10, figs. 3, 3 a. (See Agraulus oweni Meek and Hay- 
 den.) 
 
 The following species are referred by Walcott (Mon. U. S. Geol. Survey, vol. 
 8, p. 55) to Ptychoparia oweni : 
 
 Arionellus oweni Meek and Hayden, 1862 ; Am. Jour. Sci., 2d series, vol. 33, p. 74. 
 Agraulos oweni Meek and Hayden, 1864; Pal. Upper Missouri, p. 9, figs, a-c, pi. 
 
 l.fig- 4 - 
 
 Conocoryplie ( Ptychoparia ) gallatinensis Meek, 1870; 6tli Ann. Rept. U. S. Geol. 
 Survey Territories, 1872, p. 485. 
 
 Crepicephalus ( Loganella ) centralis Whitfield, 1880; Geol. Resources Black Hills, 
 D akota, p. 341, pi. 2, figs. 21-24. 
 
 [ Conocepli . ] oweni Hull, 1863 ; 16th Rept. New York State Cab. Nat. Hist., p. 155, 
 
 pi. 8, figs. 17-20. Potsdam. 
 
 I Crepicephalus ( Loganella )] planus Whitfield, 1877 ; Prelim. Rept. Pal. Black 
 
 Hills, p. 11. Potsdam. 
 
 [Crepicephalus] planus Whitfield, 1880; Geol. Black Hills Dakota, p. 343, pi. 2, 
 
 fig. 20. 
 
 ? pernasutus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8. p, 
 
 49, pi. 10, figs. 8, 8 a, b. Cambrian. 
 
 [Conocepli. ] perseus Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 153, 
 
 pi. 7, figs. 17-22 ; pi. 8, fig. 33. Potsdam. 
 
 piochensis Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 201.pl. 26, fig. 2- 
 
 2 a, b ; pi. 28, figs. 1-1 a-e. Middle Cambrian. 
 
 ? prospectensis Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 
 
 8, p. 46, pi. 9, fig. 20. Cambrian. 
 
 ? prospectensis Walcott, 1886; Bull. U. S. Geol. Survey, No. 30. p. 202, pi. 37, 
 
 fig. 5. 
 
144 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 Ptychoparia quadrangularis Whitfield. The specific name of Conoceph , quadratus 
 being preoccupied, Prof. R. P. Whitfield substitutes that of quadrangular is for 
 the species. 
 
 [Crepicepalus ( LoganeUa )] quadrans Hall and Whitfield, 1877 ; U. S. Geol. Expl. 
 
 40th Par., Palaeont., vol. 4, p. 238, pi. 2, figs. 11-13. 
 
 — — quadrans Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 199, pi. 29, figs. 4-4 
 a, b. Cambrian, 
 
 [Conoceph.] quadratus. (See Ptychoparia quadrangularis.) 
 
 [ Conoceph. ] quadratus Hartt, 1868; Acadian Geology, p. 654. St. John. 
 
 quadratus Walcott, 1884 ; Bull. U. S. Geol. Survey, No. 10 ; p. 39, pi. 5, fig. 1. 
 
 [Conoceph. f] quadratus Whitfield, 1880; Ann.Rept. Geol. Survey, Wisconsin, 
 
 1879, p. 47. 
 
 [Conoceph. ?] quadratus Whitfield, 1882; Geol. Wisconsin, vol. 4, p 180, pi. 1, 
 
 figs., 15, 16. (See Ptychoparia quadrangularis Whitfield.) 
 
 [ Conoceph .] robbi Hartt, 1868 ; Acadian Geology, p. 648. St. John. 
 
 Syn., Conoceph. formosa (Hartt) Walcott ; Bull. U. S. Geol. Survey, No. 10, p. 36. 
 
 robbi Walcott, 1884 ; Bull. U. S. Geol. Survey, No. 10, p. 36, pi. 6, figs. 1, 1 a. 
 
 [Solenopleura] robbi Matthew, 1887 ; Trans. Royal Soc. Canada, vol. 4, p. 153, pi. 
 
 2, figs. 3 a-1 ; fig. 4 a-e. 
 
 rogersi Walcott, 1884 ; Bull. U. S. Geol. Survey, No. 10, p. 47, pi. 7, fig. 2. 
 
 Lower Cambrian. 
 
 [ Conoceph .] shumardi Hall, 1863 ; 16th Kept. New York State Cab. Nat. Hist., p. 
 
 154, pi. 7, figs. 1-2 ; pi. 3, figs. 19, 32. Potsdam. 
 
 similis Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 52, pi. 
 
 10, figures. Cambrian. 
 
 similis var. rolSustus Walcott ; idem., p. 53, pi. 1, figs. 9, 9 a. 
 
 * [Conoceph.] subcoronatus Hall and Whitfield, 1877; U. S. Geol. Expl. 40th 
 
 Par., Palaeont., vol. 4, p. 237, pi. 2, fig. 1. 
 
 subcoronatus Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 205, pi. 28, 
 
 fig. 4. Middle Cambrian. 
 
 [ Conoceph. ] teucer Billings, 1861; New or little known Sil. Foss., p. 12, 
 
 fig. 16. 
 
 [Conoceph.] teucer Billings, 1861 ; Geol. Vermont, vol. 2, p. 951, fig. 356. 
 
 - [Conoceph.] teucer Billings, 1865; Pal. Foss., vol. 1, p. 13, fig. 16. 
 
 [Cenoceph.] teucer Billings, 1863; Geol. Canada, p. 286, fig. 295. 
 
 teucer Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 197, pi. 26, fig. 3. 
 
 Middle Cambrian. 
 
 [Conoceph.] tener Hartt, 1868; Acadian Geology, p. 652. St. John. 
 
 Syn., Conoceph. neglectus (Hartt) Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, 
 p. 41. 
 
 tener Walcott, 1884 ; Bull. U. S. Geol. Survey, No. 10, p. 41, pi. 5, figs. 6, 6 a, b. 
 
 [Conoceph.] thersites. (See Ptychoparia orestus Hartt.) 
 
 trilineatus. (See Atops trilineatus, Conocoryphe trilineatus, Conocepha- 
 
 lites trilineatus, Calymene beckii, Triarthrus beckii.) 
 
 [Crepicephalus ( LoganeUa )] unisulcatus Hall and Whitfield, 1877; U. S. Geol. 
 
 Expl. 40th Par., Palaeont., vol. 4, p. 216, pi. 2, figs. 22,23. Cambrian. 
 
 unisulcatus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 
 p. 58. 
 
 [Conoceph.] verucosus Whitfield, 1884 ; Bull Am. Mus. Nat. Hist., vol. 1, p. 146, 
 
 pi. 14, fig. 12. Potsdam. 
 
 [Conoceph.] vulcanus Billings, 1861; New or little known Sil. Foss., p. 14, 
 
 fig. 17. 
 
 [Conoceph.] vulcanus Billings, 1861; Geol. Vermont, vol. 2, p. 952, fig. 357. 
 
 [Conoceph ] vulcanus Billings, 1863; Geol. Canada, p. 286, fig. 296. 
 
 [Conoceph.] vulcanus Billings, 1865; Pal. Foss., vol. 1, p. 14, fig. 17. 
 
YOGDES.] 
 
 CATALOGUE OF TRILOBITES. 
 
 145 
 
 Ptychoparia vulcanus Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 196, pi. 
 26, figs. 4, 4 a. Middle Cambrian. 
 
 Compare Ptychoparia adamsi. 
 
 lConoceph.~\ winona Hall, 1863; 16th Rept‘. New York State Cab. Nat. Hist., p. 
 
 161, pi. 7, figs. 28-28. Potsdam. 
 
 [ Conocepli. ] zenkeri Billings, 1860; Canadian Naturalist, vol. 5, p. 305, fig. 4. 
 
 Quebec. 
 
 [ Conoceph .] zenkeri Billings, 1865 ; Pal. Foss., vol. 1, p. 398, fig. 375. 
 
 Remopleurides Portlock, 1843; Rept. Geol. Londonderry, etc., p. 254. 
 
 Type, Remopleurides colbii Portlock. 
 
 Syn., Caphyra Barrande, 1846; Notice Pr61im., p. 32. 
 
 Ampliytryon Corda, 1847 ; Prodr., p. 228. 
 
 affinis Billings, 1865 ; Pal. Foss., vol. 1, p. 325, fig. 313. Quebec. 
 
 canadensis Billings, 1865; Pal. Foss., vol. 1, p. 182, fig. 164. Chazy. 
 
 pander! Biilings, 1865; Pal. Foss., vol. 1, p. 293, fig. 283. Quebec. 
 
 ? schlotheimi Billings, 1865; Pal. Foss., vol. 1, p. 294, tig. 284. Quebec. 
 
 Syn., Paradoxides or Olenellus Billings, 1863; Geol. Canada, pp. 871,872. 
 
 striatulus Walcott, 1875; Cincinnati Quart. Jour. Sci., vol. 2, p. 347, fig. 27, 
 
 27 a, b. Trenton. 
 
 Sao Barrande, 1846 ; Notice Prelim. Syst. Sil. Boheme, p. 13. 
 
 ? lamottensis Whitfield, 1886; Bull. Am. Mus. Nat. Hist. New York, vol. 1, p. 
 
 334, pi. 33, figs. 9-11. Birdseye Limestone. 
 
 Shumardia Billings, 1862; Pal. Foss., vol. 1, p. 92. 
 
 Type, Shumardia granulosa Billings. 
 
 The generic name therein suggested by Mr. E. Billings for a minute Trilobite 
 includes a specimen having an expanding glabella, with two anterior side 
 nodules, simular to those of Batius pusillus Sar, the genus being allied to 
 Agnostus, differing therefrom in having a regularly ribbed pygidium, similar to 
 that of an Asaphus. Comparing Mr. E. Billings’s type, Shumardia granulosa , 
 with Conophrys salopiensis Galloway (Quart. Jour. Geol. Soc. London, vol. 33, p. 
 667, pi. 12, fig. 7), which W. C. Brogger (Sil. Etagen 2 und 3, p. 125) refers to as 
 a synonym to Battus pusillus , we fiod a similar characteristic in the glabella. 
 The pygidium of Shumardia granulosa has however a more semi- oval form, with 
 a greater number of axis rings and an additional number of ribs on the side 
 lobes. 
 
 The head of Shumardia granulosa differs from Battus pusillus in having a 
 groove, which runs from the anterior front of the glabella to the frontal margin 
 of the head, a characteristic of some species of Agnostidce ( vid . Brogger, Sil. 
 Etagen 2 und 3, pi. 1, fig. 10). 
 
 Mr. Billings remarks “that in some specimens this furrow has at the bottom 
 a small triangular tubercle, giving the glabella the appearance of having a 
 projecting angular process in the middle of its front.” I am more inclined to 
 view this triangular tubercle as a point of attachment for the muscles of the 
 jaws, and not as a process for the attachment of antennae. 
 
 Mr. E. Billings in the same book gives a description of a second species, 
 which he calls Shumardia glacialis, figured p. 283, tig. 270. The species is 
 represented with three glabella furrows, and should not be included in the 
 genus Shumardia. 
 
 If these forms are not embryonic, against which in the case of Conophrys 
 salopiensis Mr. C. Callaway dissents on account of the constant size of the 
 heads and the absence of the facial sutures amongst the larger specimens, I 
 would advocate the acceptance of the new genus Shumardia amongst the Agnos- 
 tidce for such species as Shumardia granulosa and Battus pusillus to rejilace the 
 latter generic term of Conophrys. 
 
 Bull. 63 10 
 
146 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Solenopleura Angelin, 1854; Palseont. Scand., p. 26. 
 
 Type, Solenopleura holometopa Angelin. 
 
 Diagnosis: Glabella prominent, with three distinct furrows; fixed cheeks, 
 elevated especially in the middle; front limb convex; occipital ring bearing a 
 tubercle; genal angles pointed; thorax, pleurae bluntly rounded; pygidium 
 small with few segments; surface of shell granulated with or without scat- 
 tered tubercles. 
 
 acadia Whiteaves, 1885 ; Trans. Royal Soc. Canada, vol. 3, p. 76, pi. 7, fig. 15. 
 
 Cambrian. 
 
 acadia Whiteaves, 1887 ; Trans. Royal Soc. Canada, vol. 4, p. 157, pi. 2, figs. 
 
 5 a, b, c. 
 
 acadia var. elongata Matthew, 1887 ; idem,., p. 159, pi. 1, fig. 6. 
 
 bombifrons Matthew, 1886 ; Trans. Royal Soc. Canada, vol. 2, p. 156, figs. 5-5 a b. 
 
 St. John. 
 
 communis Billings, 1874 ; Pal. Foss., vol. 2, p. 72. Potsdam. 
 
 communis Matthew, 1886 ; Trans. Royal Soc. Canada, vol. 2, p. 155, figs. 4-4 a, b. 
 
 nana Ford, 1878; Am. Jour. Sci., 3d series, vol. 15, p. 126. Potsdam. 
 
 nana Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 214, pi. 27, fig. 3. 
 
 ? nana Walcott, 1887 ; Am. Jour. Sci., 3d series, vol. 34, p. 196, pi. 1, figs. 1-1 d. 
 
 Cambrian. 
 
 orestes (Hartt) Matthew, 1887 ; Trans. Royal Soc. Canada, vol. 4, p. 154, pi. 2, 
 
 figs. 4 a-e. 
 
 Syn., robbi (Hartt) Matthew, 1887; Trans. Royal Soc. Canada, vol. 4, p. 153, 
 pi. 2, figs. 3 a-1 and figs. 4 a-e. St. John. 
 
 ? tumida Wak^ptt, 1887 ; Am. Jour. Sci., 3d series, vol. 34, p. 196, pi. 1, fig. 2, 2 a. 
 
 Cambrian. 
 
 Sphaerexochus Beyrich, 1845 ; Ueber einige bohmische Trilobiten, p. 19. 
 
 Type, Sphcerexochus minis. 
 
 canadensis Billings, 1866 ; Catalogue Sil. Foss. Anticosti, p. 64, fig. 21. 
 
 mirus (Beyrich) Roemer, 1860 ; Die Sil. Fauna W. Tennessee, p. 81, pi. 5, fig. 20. 
 
 Niagara. 
 
 parvus Billings, 1865; Pal. Foss., vol. 1, p. 180, fig. 161. Chazy and Trenton. 
 
 romingeri Hall, 1862; Geol. Rept. Wisconsin, p. 434. Niagara. 
 
 Syn., mirus Hall (not Beyrich), 1867 ; 20th Rept. New York State Cab. Nat. 
 Hist., p. 334, pi. 21, figs. 4-7. 
 
 romingeri Hall, 1867 ; 20th Rept. New York State Cab. Nat. Hist., p. 375, pi. 22, 
 
 figs. 4-7. 
 
 romingeri Hall, 1870; 20th Rept. New York State Cab. Nat. Hist., p. 425, pi. 
 
 21, figs. 4-7 (rev. ed.). 
 
 romingeri Whitfield, 1882; Geol. Wisconsin, vol. 4, p. 311, pi. 21, figs. 1-3. 
 
 romingeri ? Hall; 28th Rept. New York State Mus. Nat. Hist., p. 32, pi. 32, fig. 16. 
 
 romingeri Meek and Worthen, 1875; Geol. Survey Illinois, vol. 6, p. 510, pi. 24, 
 
 fig. 4. 
 
 Sphaerocoryphe Angelin, 1854 ; Palaeont. Scand., p. 65. 
 
 Type, Sphcerocori/phe dentata Angelin. 
 
 robustus Walcott, 1875; Cincinnati Quart. Jour. Sci., vol. 2, p. 273, figs. 18 a, b. 
 
 Trenton. 
 
 salteri Billings, 1866 ; Catalogue Sil. Foss. Anticosti, p. 63. 
 
 Symphysurus Goldfuss, 1843; Jahrb. fiir Mineral., 1843, p. 552. 
 
 — - ? goldfussi Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, 
 p. 95, pi. 12, fig. 16. Pogonip. 
 
 Telephus Barrauae, 1852; Syst. Sil. Boheme, vol. 1, p. 890. 
 
 americanus Billings, 1665; Pal. Foss., vol. 1, p 291, figs. 281. Quebec. 
 
 Terataspis Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 223. (See 
 Lichas and Acidaspis.) 
 
 grandis. (See Lichas [ Terataspis ] grandis Hall.) 
 
VOGDES.] 
 
 CATALOGUE OF TRILOBITES. 
 
 147 
 
 Terataspis eriops. (See Lichas [ Conolichas ] eriops Hall.) 
 
 Thaleops Conrad, 1843; Proc. Acad. Nat. Sci. Phila., vol. 1, p. 332. 
 
 ovatus Conrad. (See Illaenus ovatus. ) 
 
 Triarthrella Hall, 1863; 16th Rept. New York State Cab. Nat. Hist., p. 177. 
 
 auroralis Hall, 1863 ; 16th Rept. New York State Cab. Nat. Hist., p. 177, pi. 9, 
 
 fig. 13. Potsdam. 
 
 Triarthrus Green, 1832 ; Monthly Am. Jour. Geol., vol. 1, p.560 (June). Green, 1832; 
 Mon. Tril. North America, p. 86. 
 
 Type, Triarthrus beckii Green. 
 
 beckii Green, 1832; Monthly Am. Jour. Geol., vol. 1, p. 560, pi. 1, fig. 3 (June). 
 
 beckii Green, 1832; Mon. Tril. N. A., p. 86, cast 34, pi. 1, fig. 3. 
 
 beckii Harlan, 1835; Trans. Geol. Soc. Penn., vol. 1, p. 205, pi. 15, fig. 6. 
 
 Syn., [ Parqdoxides] triarthrus Harlan, 1835; Trans. Geol. Soc. Penn., vol. 1, pi. 
 p. 264, 15, fig. 5. 
 
 [Paradoxides'] arcuatus Harlan, 1835; Trans. Geol. Soc. Penn., vol. 1, p. 
 265, pi. 15, figs. 1-3. 
 
 beckii Harlan, 1835; Med. Phys. Researches, p. 400, pi., fig. 6. 
 
 Syn., [ Paradoxides} triarthrus Harlan, 1835; Med. Phys. Researches, p. 401, pi., 
 fig. 5. 
 
 [ Paradoxides ] arcuatus Harlan, 1835; Med. Phys. Researches, p. 402, pi., 
 figs. 1-3. 
 
 beckii Green, 1835 ; Suppl. Mon. Tril. N. A., p. vii. 
 
 [ Paradoxides ] beckii Hall, 1838; Am. Jour. Sci., 1st series, vol. 33, p. 142, fig. 2. 
 
 Syn., Paradoxides eatoni Hall, 1838; Am. Jour. Sci., 1st series, vol. 33, p. 142, 
 fig. 2. 
 
 beckii Green, 1838 ; Am. Jour. Sci., 1st series, vol. 33, p. 344. 
 
 beckii Mather, 1842; Geol. New York, 1st Geol. Dist., p. 390, fig. 24 (1). 
 
 beckii Emmons, 1842; Geol. New York, 2d Geol. Dist., p. 399, fig. 110 (1). 
 
 beckii Yanuxem, 1843; Geol. New York., 3d Geol. Dist., p. 57, fig. 8 (1). 
 
 beckii Hall. 1843; Geol. New York, 4th Geol. Dist., p. 504. 
 
 [ Calymene ] beckii Hall, 1847; Pal. New York, vol. 1, p. 237, pi. 64, figs. 2 a-e. 
 
 [ Calymene ] beckii Hall, 1847; Pal. New York, vol. 1, p. 250, pi. 66, figs. 2 a-k 
 
 (not pi. 67, figs. 4 a-e, Atops triliueatus). 
 
 Syn., Atops triliueatus (Emmons) Hall, 1847; Pal. New York, vol. 1, p. 237. 
 
 [ Calymene ] becki Hall, 1848 ; Am. Jour. Sci., 2d series, vol. 5, p. 322, figs. 1 a, b, 
 
 2 a-g. 
 
 becki Emmons, 1848 ; Am. Assoc. Adv. Sci., p. 17. 
 
 beckii Haldeman, 1848; Am. Jour. Sci., 2d series, vol. 8, p. 137. 
 
 beckii Emmons, 1855; Am. Geology, vol. 1, pt, 2, p. 214, pi. 15, fig. 12. 
 
 [ Calymene ] beckii Rogers, 1858; Geol. Survey Penn., vol. 2, p. 820, fig. 613. 
 
 beckii Barraude, 1861 ; Soc. Gdol. France, 2d series, p. 269, pi. 5, figs. 11, 12. 
 
 beckii Logan, 1863; Geol. Canada, p. 202, fig. 200. 
 
 beckii Miller, 1874; Cincinnati Quart. Jour. Sci., vol. 1, p. 146. 
 
 becki Walcott, 1876; Trans. Albany Inst., vol. 10, p. 23, pi. 2, figs. 1-16. 
 
 Trenton. 
 
 [Brongniartia] carcinodea Eaton, 1832; Am. Jour. Sci., 1st series, vol. 22, p. 
 
 166 (March 6). 
 
 [ Brongniartia ] carcinodea Eaton, 1832; Geol. Text Book, p. 33, pi. 1, fig. 3. 
 
 canadensis Smith, 1861 ; Canadian Jour., vol. 6, p. 275. Hudson. 
 
 fischeri Billings, 1861; Pal. Foss., vol. 1, p. 291, fig. 280. Quebec. 
 
 glaber Billings, 1859; Canadian Naturalist, vol. 4, p. 382. Utica. 
 
 glaber Billings, 1863; Geol. Canada, p. 202, fig. 198. 
 
 spinosus Billings, 1859; Canadian Naturalist, vol. 4, p. 382. Trenton. 
 
 spinosus Billings, 1863; Geol. Canada, p. 202, fig. 199. 
 
 spinosus Ami, 1882; Trans. Ottawa Nat. Club, vol. for 1882-’83, p. 88, pi. 1, figure. 
 
148 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 Triarthrus trimerus Green, 1832; Monthly Am. Jour. Geol., vol. 1, p. 560. (See Ho- 
 malonotus delphinocephalus and H. jacksoni.) 
 
 Trinucleus Lhwyd, 1698; Lithophyacii Britannici Ichnograpliia, Epistola 1. Mur- 
 chison, Silurian System, 1839, p. 659. 
 
 Sir R. I. Murchison has revived this old name of Lhwyd’s from classical feel- 
 ings, and all subsequent palaeontologists have adopted it. Lhwyd’s description 
 meant no more than the general name of Trilobite of the more modern writers, 
 and could not, except by courtesy, set aside Dr. Jacob Green’s genus Cryptolithus. 
 
 bellulus Ulrich, 1878 ; Jour. Cincinnati Soc. Nat. Hist., vol. 1, p. 99, pi. 4, fig. 15. 
 
 INuttainia ] concentrica Eaton, 1832; Geological Text Book, p. 34, pi. 1, fig. 2. 
 
 Syn., Trilobite Bigsby, 1825; Annals Lyceum Nat. Hist. New York, vol. 1, pt. 2, 
 p. 214, pi. 15, fig. 1. Trenton and Hudson. 
 
 Cryptolithus tessellatus Green, 1832; Mon. Tril. N. A., p. 73, cast 38, pi. 1, fig. 4. 
 
 Cryptolithus tessellatus Green, 1832; Monthly Am. Jour. Geol., vol. 1, pi. 1, 
 fig. 4. 
 
 concentrica Hall, 1847 ; Pal. New York, vol. 1, pp. 249, 255, pi. 65, figs. 4 a, b ; pi. 
 
 67, figs. 1 a-h. 
 
 concentrica Emmons, 1855 ; Am. Geology, vol. 1, pt. 2, p. 212, pi. 17, fig. 1. 
 
 concentrica Chapman, 1858; Canadian Jour., vol. 3, p. 514. 
 
 concentrica Billings, 1861 ; Geol. Vermont, vol. 1, p. 300, fig. 215. 
 
 concentrica Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 126. 
 
 Zacanthoides Walcott, 1887 ; Am. Jour. Sci., 3d series, vol. 36, p. 165. 
 
 Type, Zacanthoides spinosus Walcott. 
 
 [Dicellocephalus? j flagricauda White, 1874; Prelim. Rept. Invt. Foss. Geog. aud 
 
 Geol. Survey ^Vest 100th Mer., p. 12. Cambriau. 
 
 [ Dicellocephalus ? ] flagricauda White, 1877 ; U. S. Geog. and Geol. Survey West 
 
 100th Mer., vol. 4, p. 60, pi. 3, figs. 8 a, b. 
 
 [ Olenoides ] flagricauda Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 185, pi. 
 
 25, fig. 4. 
 
 flagricauda Walcott, 1888 ; Am. Jour. Sci., 3d series, vol. 36, p. 165. 
 
 [Olenoides ] levis Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 187, pi. 25, figs. 
 
 3,3 a. CambriaD. 
 
 levis Walcott, 188'8; Am. Jour. Sci., 3d series, vol. 36, p. 165. 
 
 [.Ogygiaf] spinosus Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Survey, 
 
 vol. 8, p. 63, pi. 9, fig. 22. Middle Cambrian. 
 
 [ Olenoides ] spinosus Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 184, pi. 25, 
 
 figs, 6, 6 a. 
 
 [Embolimus~\ spinosus (Rominger) Walcott, 1888; Am. Jour. Sci., 3d series, vol. 
 
 36, p. 164. 
 
 spinosus Walcott, 1888 ; Am. Jour. Sci., 3d series, vol. 36, p. 165. 
 
 [ Olenoides ] typicalis Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 183, pi. 25, 
 
 figs. 2, 2 a. Middle Cambrian. 
 
 typicalis Walcott, 1888 ; Am. Jour. Sci., 3d series, vol. 36, p. 165. 
 
PART III. 
 
 CATALOGUE OF NON-TRILOBITES. 
 
 m k ■ - - - - - - ■ - — - ■ - 
 
 149 
 
PART III 
 
 NON-TRILOBITIC GENERA AND SPECIES. 
 
 MEROSTOMATA. 
 
 EURYPTERIDiE. 
 
 Eurypterus De Kay, 1825; Annals Lyceum Nat. Hist., vol. 1, p. 375. 
 Dolichopterus Hall, 1859; Palaeont. New York, vol. 3, p. 414. 
 
 Echinognathus Walcott, 1882; Am. Jour. Sci. r 3d series, vol. 23, p. 213. 
 Adelophthalmus Jordan and Meyer, 1854; Crust. Steinkohl. Saarb., p. 8. 
 Glyptoscorpius Peach, 1880; Trans. Royal Soc. Edinb., vol. 30, p. 516. 
 Arthropleura Jordan and Meyer, 1854 ; Crust. Steinkohl. Saarb., p. 13. 
 
 PTERYGOTIDiE. 
 
 Pterygotus Agassiz, 1844; Mon. Poissons Foss., note, p. xix. 
 
 Slimonia Page, 1856 ; Advance Text-Book Geology, p. 135. 
 
 Stylonurus Page, 1856 ; Advance Text-Book Geology. 
 
 SYNZIPHOSURA. 
 
 Acanthotelson Meek and Worthen, 1865 ; Proc. Acad. Nat. Sci. Phila., vol. 17, p. 46 
 Geol. Survey Illinois, vol. 2, 1866, p. 399. 
 
 4 
 
 XIPHOSURA. 
 
 CYCLID.®. 
 
 Cyclus De Koninck, 1841 ; M6m. Acad. Sci. Belgique, vol. 14, p. 13. 
 
 Dipeltis Packard, 1885; American Naturalist, vol. 19, p. 293. 
 
 BUNODIDvE. 
 
 Bunodes Eichwald, 1854 ; Beitriige Geol. u. Pal. Russ., p. 131. 
 
 Hemisapis Woodward, 1865; Quart. Jour. Geol. Soc. London, vol. 21, p. 490. 
 Exapinurus Nieszkowski, 1859; Archiv Nat. Liv-, Esth- u. Kurl., vol. 1, p. 380. 
 Pseudoniscus Neiszkowski, 1859; Archiv Nat. Liv-, Esth- u. Kurl., vol. 1, p. 381. 
 
 LIMULID^E. 
 
 Belinurus Koenig, 1820 ; leones Foss. Sec tiles, pi. 18, fig. 230. 
 
 Prestwichia Woodward, 1887 ; Quart. Jour. Geol. Soc. London, vol. 23, p. 32. 
 
 151 
 
152 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63 . 
 
 Limulus Muller, 1785; Entomostraca, etc.,p. 124. 
 
 Protolimulus Packard, 1886; Mem. Nat. Acad. Sci., vol. 3, p. 150. 
 
 Neolimulus Woodward, 1868; Geol. Mag., vol. 5, p. 1. 
 
 PHYLLOPODA. 
 
 CERATIOCARIDiE. 
 
 Hymenocaris Salter, 1852; Rept. 22d Meeting Brit. Assoc. Adv. Sci., Trans. Sec., 
 p. 56. 
 
 Ceratiocaris McCoy, 1849 ; Annals Mag. Nat. Hist. London, 2d series, vol. 4, p. 412. 
 Echinocaris Whitfield, 1880; Am. Jour. Sci., 3d series, vol. 19, p. 34. 
 
 Didyocaris Salter, 1860 ; Annals Mag. Nat. Hist. London, 3d series, vol. 5, p. 161. 
 Dithyocaris (Scouler) Portlock ; Geol. Rept. Londonderry, etc., 1843, p. 313. 
 Protocaris Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 50. 
 
 Elymocaris Beecher, 1884 ; 2d Geol. Survey Penn., vol. PPP., p. 13. 
 
 Tropidocaris Beecher, 1884; 2d Geol. Rept. Penn., vol. PPP., p. 15. 
 
 Physocaris Salter, 1860 ; Annals Mag. Nat. Hist. London, 3d series, vol. 5, p. 159. 
 Phasganocaris Novak, 1886 ; Sitzungsb. bohm. Gesell., 1886, p. 498. 
 
 Acanthocaris Peach, 1882; Trans. Royal Soc. Edinb., vol. 30, p. 511. 
 
 DISCINOCARHLE. 
 
 Discinocaris Woodward, 1866; Quart. Jour. Geol. Soc. London, vol. 22, p. 504. 
 Spathiocaris Clarke, 1882; Am. Jour. Sci., 3d series, vol. 23, p. 477. 
 
 Pholadocaris Woodward, 1882; Geol. Mag., decade 3, vol. 9, p. 388. 
 
 Ellipsocaris Woodward, 1882 ; Geol. Mag., decade 3, vol. 9, p. 444. 
 
 Lisgocaris Clarke, 1882; Am. Jour. Sci., 3d series, vol. 23, p. 478. 
 
 Cardiocaris Woodward, 1882 ; Geol. Mag., decade 3, vol. 9, p. 386. 
 
 Dipterocaris Clarke, 1883 ; Am. Jour. Sci., 3d series, vol. 23, p. 121. 
 
 Pterocaris Barrande, 1872 ; Syst. Sil. Boheme, vol. 1, suppl., p. 464. 
 
 Crescentella Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 507. 
 Aptychopsis Barrande, 1872 ; Syst. Sil. Boheme, vol. 1, suppl., p. 455. 
 
 Peltocaris Salter, 1863 ; Quart. Jour. Geol. Soc. London, vol. 19, p. 87. 
 
 Pinnocaris Etheridge, 1878; Proc. Royal Phys. Soc., Edinb., vol. 4, p. 167. 
 Ptychocaris Novak, 1885; Sitzungsb. bohm. Gesell., 1885, p. 343. 
 
 RHINOCARHLE. 
 
 Rhinocaris Clarke, 1888 ; Palaeont. New York, vol. 7, p. lviii. 
 
 Colpocaris Meek, 1871; Proc. Acad. Nat. Sci. Phila., vol. 23, p. 334. 
 
 Solenocaris Meek, 1871 ; Proc. Acad. Nat. Sci. Phila., vol. 23, p. 335. Name should 
 be changed, preoccupied by J. Young. See Strigocaris. 
 
 Mesothyra Hall, 1888 ; Palaeont. New York, vol. 7, pp. lvi, 187. 
 
 Sacocaris Salter, 1868; Proc. Geol. Poly tech. Soc., vol. 4, p. 588. 
 
 Lingulocaris Salter, 1866 ; Mem. Geol. Survey, vol. 3, pp. 252, 253, and 294. 
 Solenocaris Young, 1868 ; Proc. Nat. Hist. Soc. Glasgow, vol. 1, p. 171. 
 
 Rostrocaris Kinnear, 1887; Trans. Edinb. Geol. Soc., vol. 5, p. 417. 
 
 Caryocaris Salter, 1863; Quart. Jour. Geol. Soc. London, vol. 19, p. 139. 
 Entomidella Jones, 1873 ; Annals Mag. Nat. Hist., London, 4th series, vol. 11, p: 416. 
 Arch^cocaris Meek, 1872 ; Proc. Acad. Nat. Sci. Phila., vol. 23, p. 335. 
 
 Myocaris Salter, 1864 ; Quart. Jour. Geol. Soc. London, vol. 20, 1864, p. 292. 
 Estheria Ruppell, 1857 ; Mus. Senckenberg, vol. 2, p. 119. 
 
 Leaia Jones, 1882 ; Mon. Fossil Estheria, p. 115. 
 
 Schizodiscus Clarke, 1888; Palaeont. New York, vol. 7, p. 207. 
 
VOGDES. ] 
 
 CATALOGUE OF NON-TRILOBITES. 
 
 153 
 
 BIVALVED ENTOMOSTRACA. 
 
 CYPRIDINID^E. 
 
 Cypridina Milne-Ed wards, 1838; Lamarck’s Anim. s. Vert., vol. 5, p. 178. 
 Cypridinella Jones and Kirkby, 1874; Mon. Carboniferous Eutom., p. 21. 
 Cypridellina Jones and Kirkby, 1874; Mon. Carboniferous Entom., p. 25. 
 
 Sulcuna Jones, 1873; Quart. Jour. Geol. Soc. London, vol. 29. p. 411. 
 
 , Cyprella De Koninck, 1841 ; M6m. Acad. Royale Bruxelles, vol. 14, p. 19. 
 Bradycinetus Sars, 1865 ; Oversigt af Norges Marine Ostracoder. 
 
 Philomedes Lilljeborg, 1853 ; Crust, in Scania Occurrentibus, p. 175. 
 
 Rhombina Jones and Kirkby, 1874 ; Mon. Carboniferous Entom., p. 43. 
 
 ENTOMOCONCHIDiE. 
 
 Entomoconchus McCoy, 1839; Jour. Geol. Soc. Dublin, vol. 2, p. 91. 
 
 Offa Jones and Kirkby, 1874; Mon. Carboniferous Entom., p. 53. 
 
 POLYCOPID.E. 
 
 Polycope Sars, 1865 ; Oversigt af Norges Marine Ostracoder. 
 
 ENTOMIDID^E. 
 
 Entomis Jones, 1861 ; Mem. Geol. Survey Scotland, Expl. map 32, p. 137. 
 
 CYTHERELLHLE. 
 
 Cytherella Jones and Bosquet, 1848 and 1852. 
 
 Cytherellina Jones and Holl, 1869; Annals Mag. Nat. Hist., London, 4th series, 
 vol. 3, p. 215. 
 
 Cytherina Lamarck, 1818; Animaux sans Vert., vol. 5, p. 125. 
 
 JEchmixa Jones and Holl, 1869 ; Annals Mag. Nat. Hist., London, 4th series, vol. 3, 
 p. 217. 
 
 LEPERDITIDiE. 
 
 Leperditia Rouault, 1851 ; Bull. Soc. G6ol. France, 2d series, vol. 8, p. 377. 
 
 Bernix Jones, 1884 ; Proc. Berwickshire Nat. Club, vol. 10, p. 316. 
 
 Isochilin a Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 248. 
 Primitia Jones and Holl, 1865 ; Annals Mag. Nat. Hist., Loudon, 3d series, vol. 16, 
 p. 416. 
 
 Beyrichia McCoy, 1846 ; Synopsis Sil. Foss. Ireland, p. 57. 
 
 Beyrichiella Jones and Kirkby, 1886 ; Geol. Mag., n. s., decade 3, vol. 3, p. 438. 
 Kirkbya Jones, 1869; Annals Mag. Nat. Hist., London, 4th series, vol. 3, p. 223. 
 
 Moo rea Jones and Kirkby, 1867 ; Annals Mag. Nat. Hist., London, 4th series, vol. 3, 
 p. 225. 
 
 Phreatura Jones and Kirkby, 1886; Quart. Jour. Geol. Soc. London, vol. 42, p. 507. 
 
 I Strepula Jones and Holl, 1886 ; Annals Mag. Nat. Hist., London, 5th series, vol. 17, 
 
 p. 403. 
 
 | Bollia Jones and Holl, 1886 ; Annals. Mag. Nat. Hist., London, 5th series, vol. 17, 
 [ p. 360. 
 
 B Kl(EDINIA Jones and Holl, 1886 ; Anuals Mag. Nat. Hist., London, 5th series, vol. 17, 
 p. 362. 
 
 ri Beyrichiopsi8 Jones and Kirkby, 1886 ; Geol. Mag., decade 3, vol. 3, p. 434. 
 
 II Aparchites Jones, 1889; Annals Mag. Nat. Hist., 6th series, vol. 3, p. 385. 
 Primitopsis Jones, 1887; Notes on some Sil. Ostracoda from Gothland, p. 5. 
 
 ; 
 
154 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 Placentura Jones and Holl, 1886; Annals Mag. Nat. Hist., London, 5th series, vol. 
 17, p. 407. 
 
 Kyamodes Jones, 1888; Annals Mag. Nat. Hist., London, 6th series, vol. 2, p. 295. 
 Cyprosis Jones, 1881 ; Geol. Mag., decade 2, vol. 8, p. 338. 
 
 Cyprosina Jones, 1881 ; Geol. Mag., decade 2, vol. 8, p. 338. 
 
 Octonaria Jones, 1887; Annals Mag. Nat. Hist., London, 5th series, vol. 19, p. 404. 
 
 CYPRIDJE. 
 
 Aglaia Brady, 1867; Challenger Exped.,Rept. on Ostracoda, p. 33. 
 
 Candona Baird, 1850 ; History Brit. Entomostraca, p. 159. 
 
 ARGILL.ECIA Sars, 1865 ; Ofversigt af Norges Marine Ostracoder. 
 
 Macrocypsis Brady, 1867 ; Intellectual Observ., vol. 12, p. 119. 
 
 Bathocypsis Brady, 1880; Challenger Exped., Rept. on Ostracoda, p. 45. 
 
 Bairdia McCoy, 1844 ; Synopsis Carboniferous Foss. Ireland, p. 164. 
 
 DARWINULIDiE. 
 
 Darwinula (Brady and Robertson) Jones, 1885; Quart. Jour. Geol. Soc., vol. 41, p. 
 346. Name changed from preoccupied term Darwinella (Ann. Mag. Nat. Hist., 
 4th series, vol. 9, 1872, p. 50). 
 
 CYTHERIDiE. 
 
 CYTHERE Muller, 1785 ; Entomostraca, etc., p. 64. 
 
 Xestoleberis Sars, 1865 ; Ofversigt af Norges Marine Ostracoder, p. 68. 
 Bythocythere Sars, 1865; Ofversigt af Norges Marine Ostracoder. 
 
 Carbonia Jones, 1870; Geol. Mag., vol. 7, p. 218. 
 
 Youngia Jones and Kirkby, 1886; Quart. Jour. Geol. Soc. London, vol. 42, p. 507. 
 Thlipeura Jones and Holl, 1869 ; Annals Mag. Nat. Hist., London, 4th series, vol. 3, 
 p. 213. 
 
 Bursulella Jones, 1887 ; Notes on some Sil. Ostracoda from Gothland, p. 7. 
 Aristozoe Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 474. 
 
 Orozoe Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 537. 
 
 Callizoe Barraude, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 503. 
 
 Zonozoe Barrande, 1872 ; Syst. Sil. Boheme, vol. 1, suppl., p. 554. 
 
 Hippa Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 516. 
 
 Bolbozoe Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 500. 
 
 Elpe Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 510. 
 
 Nothozoe Barrande, 1872 ; Syst. Sil. Boheme, vol. 1, suppl., p. 536. 
 
 Caryon Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 505. 
 
 Cryptozoe Packard, 1888; Proc. Acad. Nat. Sci. Phila., 1888, p. 381. 
 
 Cytheropsis (McCoy) Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 508. 
 
 CIRRIPEDJE. 
 
 Plumulites Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 565. 
 
 Strobilepis Clarke, 1888; Palseont. New York, vol. 7, p. 212. 
 
 Paleocreusia Clarke, 1888 ; Palseont. New York, vol. 7, p. 210. 
 
 Protobalanus Whitfield, 1888; Palseont. New York, vol. 7, p. lxii; Bull. Am. Mus. 
 Nat. Hist., vol. 2, 1889, p. 66. 
 
 Turrilepas Woodward, 1865; Quart. Jour. Geol. Soc. London, vol. 21, p. 489. 
 
 DECAPODA. 
 
 Anthrapalemon Salter, 1861 ; Quart. Jour. Geol. Soc. London, vol. 17, p. 529. 
 Paleopalemon Whitfield, 1880; Am. Jour. Sci., 3d series, vol. 19, p. 40. 
 Crangopsis Salter, 1863; Quart. Jour. Geol. Soc. London, vol. 19, p. 80. 
 Pseudo-Galathea Peach, 1882; Trans. Royal Soc. Edinb., vol. 30, p. 573. 
 
VOGDEB.] 
 
 CATALOGUE OF NON-TR1LOBITES. 
 
 155 
 
 SCHIZOPODA. 
 
 Gampsonyx Meyer, 1847 ; Verhandl. Nat. Vereins Preuss., vol. 4, p. 86. 
 Pal^eocaris Meek and Worthen, 1865 ; Proc. Acad. Nat. Sci. Phila., p. 48. 
 Nkctotelson Brocchi, 1880 ; Bull. Soc. G6ol. France, 3d series, vol. 8, p. 10. 
 
 AMPHIPODA. 
 
 Diplostylus Salter, 1863 ; Quart. Jour. Geol. Soc. London, vol. 19, p. 76. 
 
 STEOMAPODA. 
 
 Amphipeltis Salter, 1863 ; Quart. Jour. Geol. Soc. London, vol. 19, p. 75. 
 
CATALOGUE OF NORTH AMERICAN PALEOZOIC CRUSTACEA— NON- 
 
 TRILOBITA. 
 
 (Current generic names in bold face ; synonyms in Italic .] 
 
 Acanthotelson Meek and Worfchen, 1865 ; Proc. Acad. Nat. Sci. Phila., vol. 17, p. 46 • 
 Geol. Survey Illinois, vol. 2, 1866, p. 299. 
 
 Type, A. stimsoni. 
 
 eveni Meek and Worfchen, 1868 ; Am. Jour. Sci., 2d series, vol. 46, p. 28. 
 
 . „ Coal Measures, 
 
 eveni Meek and Worthen, 1868 ; Geol. Survey Illinois, vol. 3, p. 551, figs. a-d. 
 
 ! eveni White, 1884 ; 13th Rept. Dept. Geol. Nat. Hist. Indiana, p. 177, pi. 38, figs. 
 
 I eveni Packard, 1886; Mem. Nat. Acad. Sci., vol. 3, p. 125. 
 
 | inequalis. (See Falaeocaris typus.) 
 
 ? magister Packard, 1886 ; Mem. Nat. Acad. Sci., vol. 3, p. 127, pi. 1 fig. 2 • pi. 
 
 2, figs. 4, 5. Carboniferous, 
 
 stimpsoni Meek and Worthen, 1865; Proc. Acad. Nat. Sci. Phila.. vol. 17, p. 47. 
 
 . . Coal Measures, 
 
 stimpsoni Meek and Worthen, 1866 ; Geol. Survey Illinois, vol. 2, p. 401 pi 32 
 figs. 6, 6 a-f. ’ 
 
 stimpsoni Meek and Worthen, 1868 ; Geol. Survey Illinois, vol. 3, p. 549, figs, a, b. 
 stimpsoni Woodward, 1881 ; Geol. Mag., decade 2, vol. 8, p. 533, pi. 14, fig. 4. 
 stimpsoni White, 1884 ; 13th Rept. Dept. Geol. Nat. Hist. Indiana, p. 176 pi. 37 
 figs. 4, 5. ’ ' ’ 
 
 stimpsoni Packard, 1886; Mem. Nat. Acad. Sci., vol. 3, p. 124. 
 
 Packard considers this species to be the young of Acanthotelson eveni. 
 JEchmina Jones and Holl, 1887; Annals Mag. Nat. Hist., 5th series, vol. 3, p. 217. 
 byrnesi (Miller) Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 12, pi. 3, figs. 
 
 „ * , _ Cincinnati. 
 
 b or other references, see Leperditia byrnesi Miller. 
 
 spinosa (Hall) Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 11, pi. 3, fi g8 . 
 
 Niagara 
 
 For other references, see Cytherina spinosa Hall. 
 
 Amphipeltis Salter, 1863 ; Quart. Jour. Geol. Soc. London, vol. 19, p. 75. 
 
 paradoxus Salter, 1863; Quart. Jour. Geol. Soc. London, vol. 19, p. 76, figs. 11 
 
 ’ , _ Devonian, 
 
 paradoxus Dawson, 1868; Acadian Geology, p. 523, fig. 180. 
 
 * paradoxus Salter and Woodward ; Chart of Fossil Crustacea, pi. 3 fi«- 3 
 Anthracovetes Meek and Worthen, 1868; Am. Jour. Sci., 2d eeriee, vol. 46 p 21 
 
 mazonensis Meek and Worthen. (See Eurypterus mazonensis ) 
 
 Anthrapaleemon Salter, 1861; Quart. Jour. Geol. Soc. London, vol. 17 p. 52». 
 
 Type, A. yrossarii Salter. ’ 
 
 gracilis Meek and Worthen, 1865 ; Proc. Acad. Nat. Sci. Phila., vol. 17, p. 50. 
 
 ... . Coal Measures. 
 
 gracilis Meek and Worthen, 1866; Geol. Survey Illinois, vol. 2, p. 407 pi 32 
 figs. 4 a, b, c. r ’ ’ 
 
 157 
 
158 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Anthrapaleemon gracilis Meek and Worthen, 1868; Geol. Survey Illinois, vol. 3, p. 
 
 554, figs, a, b. 
 
 gracilis White, 1884 ; 13th Rept. Dept. Geol. Nat. Hist. Indiana, p. 180, pi. 38, 
 
 figs. 8, 9. 
 
 gracilis Packard, 1885 ; American Naturalist, vol. 19, p. 880. 
 
 gracilis Packard, 1886; Mem. Nat. Acad. Sci., vol. 3, p. 135, pi. 4, figs. 1,2, 3, 5, 
 
 6; pi. 7, figs. 3-6. 
 
 [Palceocarabu8~\ hillianus Dawson, 1878; Geol. Mag., vol. 4, p. 56, fig. 1. 
 
 Coal Measures. 
 
 [ Palceocarabus ] hillianus Dawson, 1878; Suppl. Acadian Geology, p. 55, fig. 
 
 10 . 
 
 Aparchites Jones, 1889; Annals Mag. Nat. Hist., 6th series, vol. 3, p. 385. 
 
 minutissimus (Hall) Ulrich, 1889; Contributions Micro-Palseont., pt. 2, p. 49. 
 
 For other references, see Leperditia [ Isochilina ] minutissima Hall. Hudson. 
 
 unicornis Ulrich, 1889 ; Contributions Micro-Palseont., pt. 2, p. 50, pi. 9, fig. 11. 
 
 For other references, see Leperditia unicornis. Hudson. 
 
 Aptychopsis Barrande, 1872; Syst. Sil. Boheme, vol. 1, suppl., p. 436. 
 Archaeocaris Meek, 1871 ; Proc. Acad. Nat. Sci. Phila., vol. 23, p. 335. 
 
 vermiformis Meek, 1871 ; Proc. Acad. Nat. Sci. Phila., vol. 23, p. 335. 
 
 Carboniferous. 
 
 Aristozoe Barrande, 1872 ; Syst. Sil. Boheme, suppl., vol. 1, p. 474. 
 
 rotundata Walcott, 1887 ; Am. Jour. Sci., 3d series, vol. 34, p. 193, pi. l,fig. 9. 
 
 Cambrian. 
 
 troyensis (Ford) Walcott, 1887 ; Am. Jour. Sci., 3d series, vol. 34, p. 193, pi. fig. 
 
 8. Cambrian. 
 
 [ Leperditia ] troyensis Ford, 1873 ; Am. Jour. Sci., 3d series, vol. 6, p. 138. 
 
 Aristozoe sp. Shaler and Foerste, 1888; Bull. Mus. Comp. Zoology, vol. 16, p. 35, pi. 
 
 2, fig. 18. Cambrian. 
 
 Belinurus Koenig, 1820 ; leones. Foss. Sectiles, p. 18, fig. 230 ; Baily, Annals Mag. Nat. 
 
 Hist., London, 3d series, vol. 11, 1863. 
 
 dance Meek and Worthen. (See Frestwichia danae.) 
 
 laccei Packard, 1885 ; American Naturalist, vol. 19, p. 292. Carboniferous. 
 
 laccei Packard, 1886; Mem. Nat. Acad. Sci., vol. 3, p. 149, pi. 5, fig. 5. 
 
 Beyrichia McCoy, 1846; Silurian Foss. Ireland, p. 58. 
 
 Type, Beyrichia Iclodeni McCoy. 
 
 eequilatera Hall, 1860; Canadian Naturalist, vol. 5, p. 158, fig. 20. Silurian. 
 
 aequilatera Dawson, 1868; Acadian Geology, p. 609, fig. 217. 
 
 aequilatera Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 18, pi. 2, fig. 6. 
 
 atlantica Billings, 1865; Pal. Foss., vol. 1, p. 300. Quebec. 
 
 bela Walcott, 1883; Description New Species Trenton Group, p. 7, pi. 17, figs. 11, 
 
 11 a. Trenton. 
 
 bela Walcott, 1884; 35th Rept. New York State Mus. Nat. Hist., p. 213, pi. 17, 
 
 figs. 11, 11 a. 
 
 buchiana ? Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 16, pi. 3, fig. 25. 
 
 Cincinnati. 
 
 chambersi Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 234, fig. 27. 
 
 Hudson. 
 
 chambersi Hall and Whitfield, 1875 ; Pal. Ohio, vol. 2, p. 104, pi. 4, figs. 11, 12. 
 
 ciliata Emmons, 1855 ; American Geology, pt. 2, p. 219, fig. 74 c. Hudson. 
 
 ciliata Miller, 1875; Cincinnati Quart. Jour. Sci., vol. 2, p. 351. 
 
 ciliata Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 19, pi. 3, figs. 12-16 ; pi. 4, 
 
 figs. 16-18. 
 
 Syn., Beyrichia tumifrons Hall. 
 
 cincinnatiensis Miller, 1875; Cincinnnati Quart. Jour. Sci., vol. 2, p. 350, fig. 25. 
 
 Hudson. 
 
VOGDES J 
 
 CATALOGUE OF NON-TRILOBITES. 
 
 159 
 
 Beyrichia cincinnatiensis Walcott, 1876 ; Trans. Albany Inst., vol. 10, p. 23. 
 
 clarkei Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 17, wood-cut, fig. 2. 
 
 Lower Helderberg. 
 
 clathrata Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p.242, 
 
 pi. 9, fig. 1. Niagara. 
 
 dagon Clarke, 1885 ; Bull. U. S. Geol. Survey, No. 16, p. 29, pi. 2, figs. 6, 7. 
 
 Genesee. 
 
 decora Billings, 1866 ; Catalogue Sil. Foss. Anticosti, p. 67. 
 
 duryi Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 232, figs. 24, 25. 
 
 Hudson. 
 
 fcetoidea White and St. John, 1868 ; Trans. Chicago Acad. Sci., vol. 1, p. 126, figs. 
 
 11 a, b. Niagara. 
 
 granulosa Hall, 1876 ; 28th Rept. New York State Mus. Nat. Hist., Doc. Ed. Expl., 
 
 pi. 32, fig. 4. Niagara. 
 
 granulosa Hall, 1876 ; 28th Rept. New York State Mus. Nat. Hist., p. 186, pi. 32, 
 
 fig. 4. 
 
 granulosa Hall, 1883 ; 11th Annual Rept. Dept. Geol. Nat. Hist. Indiana, p. 331, 
 
 pi. 34, fig. 4. 
 
 • granulosa Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 15, pi. 1, fig. 3. 
 
 granulata Hall, 1859; Pal. New York, vol. 3, p. 377, pi. 79 b, figs. 1 a-d. 
 
 Lower Helderberg. 
 
 halli Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 15, pi. 4, fig. 21. 
 
 Waterlirae. 
 
 hamiltonensis Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 19, pi. 2, fig. 3. 
 
 Hamilton. 
 
 jonesii Dawson, 1868; Acadian Geology, p. 313, fig. 132. Carboniferous. 
 
 laid. (See Bollia lata Vanuxem.) 
 
 lithof actor White and St. John, Prelim. Notice New Genera and Species Foss., 
 
 May 8, 1867, p. 2. 
 
 Changed to Beyrichia petrifactor, which see. Coal Measures. 
 
 lithofactor var. velata ; idem., p. 2. (See Beyrichia petrifactor var. velata.) 
 
 logani Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 244, pi. 9, 
 
 figs. 6-10. Chazy. 
 
 logani Jones, 1858; Geol. Survey Canada, decade 3, p. 91, pi. 11, figs. 1-5. 
 
 logani var. remiformis Jones, 1858; Geol. Survey Canada, decade 3, p. 91, pi. 
 
 11, fig. 1. 
 
 logani var. leperditoides Jones, 1858; Geol. Survey Canada, decade 3, p. 91, pi. 
 
 11, fig. 5. 
 
 maccoyana Jones, 1855; Annals Mag. Nat. Hist., London, 2d series, vol. 16, p. 
 
 88, pi. 5, fig. 14. Onondaga. 
 
 maccoyana Jones, 1858 ; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 252, 
 
 pi. 10, fig. 15. 
 
 maccoyana Jones, 1858; Geol. Survey Penn., vol. 2, p. 834, fig. 695. 
 
 notata. (See Klcedenia notata (Hall) Jones.) 
 
 nova scotica Jones and Kirkby, 1884; Geol. Mag., 5th series, vol. 1, p. 337, pi. 
 
 12, figs. 5, 6. Carboniferous. 
 
 sp ? Dawson, 1868; Acadian Geology, p. 256, fig. 78 c. 
 
 [ Primitia ] occidentals Walcott, 1884 ; Pal. Eureka Dist., Mon. U. S. Geol. Sur- 
 vey, vol. 8, p. 104, pi. 17, figs. 4, 4 a. Devonian. 
 
 oculifera Hall, 1871 ; Pamphlet Cincinnati Group, p. 8. Hudson. 
 
 oculifera Hall, 1872; 24th Rept. New York State Mus. Nat. Hist., p. 232, pi. 8, 
 
 figs. 9, 10. 
 
 oculifera Hall and Whitfield, 1875; Pal. Ohio, vol. 2, p. 103, pi. 4, figs. 9, 10. 
 
 :J oculifera Miller, 1874; Cincinnati Quart. Jour. Sci., vol. 1, p. 118. 
 
 oculifera Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 21, pi. 4, figs. 19 a, b, 20. 
 
160 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull. 63. 
 
 Beyrichia oculina Hall, 1859; Pal. New York, vol. 3, p. 378, pi. 79 b, figs. 2 a-e. 
 
 Lower Helderberg. 
 
 oculina Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 16, pi. 1, fig. 4. 
 
 parasitica (Hall) Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 16, wood-cut. 
 
 For other references, see Leperditia parasitica . 
 
 pennsylvanica Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, 
 
 p. 253, pi. 10, fig. 16-18. Onondaga. 
 
 pennsylvanica Jones, 1858; Geol. Survey Penn., vol. 2, p. 834, fig. 696. 
 
 persulcata Ulrich, 1879; Jour. Cincinnati Soc. Nat. Hist., vol. 2, p. 12, pi. 7, 
 
 fig. 6. Hudson. 
 
 petrifactor White and St. John; Trans. Chicago Acad. Sci., vol. 1, p. 125. 
 
 petrifactor var. velata; idem., p. 126. 
 
 plagosa Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 243, 
 
 pi. 9, fig. 2. Niagara. 
 
 punctulifera Hall, 1861 ; Des. New Species Fossils, p. 83. Hamilton. 
 
 punctulifera Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 111. 
 
 pustulosa Hall, 1860; Canadian Naturalist, vol. 5, p. 157, fig. 19. Silurian. 
 
 pustulosa Dawson, 1868 ; Acadian Geology, p. 608, fig. 216. 
 
 pustulosa Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 18, pi. 2, fig. 1 a-c. 
 
 Referred to Beyrichia tuherculata Boll var. pustulosa Hall. 
 
 quadrilirata Hall and Whitfield, 1875; Pal. Ohio, vol. 2, p. 105, pi. 4, figs. 6, 7. 
 
 Hudson. 
 
 quadrilirata Miller, 1875; Cincinnati Quart. Jour. Sci., vol. 2, p. 351. (See 
 
 Strepula quadrilirata.) 
 
 regularis Emmons, 1855 ; American Geology, pt. 2, p. 219, fig. 74 b. Hudson. 
 
 regularis Miller, 1875’; Cincinnati Quart. Jour. Sci., vol. 2, p. 351. 
 
 This species is placed as a synonym to Bollia lata by Jones (1890, Quart. 
 Jour. Geol. Soc., vol. 46, p. 13). 
 
 remiformis Jones, 1858; Geol. Survey Canada, decade 3, p. 91, pi. 11, fig. 1. 
 
 Chazy. 
 
 richardsoni Miller, 1874; Cincinnati Quart. Jour. Sci., vol. 1, p. 347, fig. 40. 
 
 Hudson. 
 
 rugulifera Jones, 1858; Annals Mag. Nat. Hist. London, 3d series, vol. 1, p. 242, 
 
 pi. 9, fig. 4. Niagara. 
 
 sigillata Jones, 1858; Annals Mag. Nat. Hist., London, vol. 1, p. 242, pi. 9, fig. 5. 
 
 Niagara. 
 
 simplex (Jones) Emmons, 1855 ; American Geology, vol. 1, pt. 2, p. 218, fig. 74 a. 
 
 {Cythei'ina'] spinosa Hall, 1852; Pal. New York, vol. 2, p. 317, pi. 67, figs. 17-20. 
 
 (See .ffichmina spinosa.) Niagara. 
 
 striato-marginatus Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 233, fig. 
 
 26. 
 
 This species is referred to a new genus. (See Eurychilinda striatomar- 
 
 ginatus.) Hudson. 
 
 symmetrica Hall, 1852; Pal. New York, vol. 2, p. 317, pi. 67, fig. 16. (See Bollia 
 
 symmetrica.) Niagara. 
 
 trisulcata Hall, 1859 ; Pal. New York, vol. 3, p. 381, pi. 79, figs. 5 a, b. 
 
 Lower Helderberg. 
 
 trisulcata Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 14, pi. 1, fig. 2. 
 
 tumifrons Hall, 1871 ; Des. New Species Foss. Hudson River Group, p. 7. 
 
 Hudson. 
 
 tumifrons Hall, 1872 ; 24th Rept. New York State Mus. Nat. Hist., p. 231, pi. 8, 
 
 fig. 11. 
 
 tumifrons Hall and Whitfield, 1875 ; Pal. Ohio, vol. 2, p. 102, pi. 4, fig. 8. 
 
 tumifrons Miller, 1874; Cincinnati Quart. Jour. Sci., vol. 1, p. 119. 
 
 This species is classed by Jones 1890, Quart. Jour. Geol. Soc., vol. 46, p. 19, 
 as synonymous to Beyrichia ciliata Emmons. 
 
VOGUES. 
 
 CATALOGUE OF N ON-TR1LOBXTES 
 
 161 ' 
 
 Beyrichia venusta Billings, 1866; Catalogue Silurian Fossils Anticosti, p. 68. 
 Bollia Jones aud Holl, 1886; Annals Mag. Nat. Hist., 5th series, London, vol. 17, p. 
 360. 
 
 \_Agnostu8'] latus Vanuxem, 1842; Geol. New York, 3d Geol. Dist.,p. 80. 
 
 Clinton. 
 
 [ Beyrichia ] lata Hall, 1852; Pal. New York, vol. 2, p. 301, pi. A 66, figs. 10 a-c. 
 
 [ Beyrichia ] lata Jones, 1858; Notes on Palaeozic Entomostraca, No. 2, p. 168, pi. 
 
 6, fig. 13. 
 
 lata Jones, 1800; Quart. Jour. Geol. Soc., vol. 46, p. 12, pi. 3, figs. 1-3. 
 
 [ Beyrichia ] symmetrica Hall, 1852 ; Pal. New York, vol. 2, p. 317, pi. 67, fig. 16. 
 
 Niagara. 
 
 symmetrica Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 12. 
 
 This species is closely allied to Bollia lata. 
 
 ungula (Claypole MS.) Jones, 1889; American Geologist, vol. 4, p. 338, pi. 
 
 fig. 10-13. Marcellus. 
 
 Bythocypris Brady, 1880; Challenger Exped., Rep. Ostracoda, p. 45. 
 
 cylindrica (Hall) Ulrich, 1889; Contributions Micro-Palseont., pt. 2, p. 48, pi. 
 
 9, fig. 6. Trenton and Hudson. 
 
 For other references, see Leperditia \_Isochilina ] cylindrica Hall. 
 
 favulosa Jones, 1889; American Geologist, vol. 4, p. 338, pi. figs. 2 a-c. 
 
 Marcellus. 
 
 oviformis Jones, 1889 ; American Geologist, vol. 4, p. 340, pi. figs. 3 a-c. 
 
 Lower Helderberg. 
 
 Carbonia Jones and Kirkby, 1879; Annals Mag. Nat. Hist., London, 5th series, 
 vol. 4, p. 28. 
 
 ? bairdioides (?) Jones and Kirkby, 1884 ; Geol. Mag., 5th series, vol. 1, p. 358, 
 
 pi. 12, figs. 8 a-d. Carboniferous. 
 
 Syn., Bairdia sp. ? Dawson, 1868; Acadian Geology, p. 206, figs. 48 a (?). 
 
 [ Cyth ere ? (Carbonia)] bairdiodes Jones and Kirby, 1879 ; Annals Mag. Nat. Hist., 
 
 London, 5th series, vol. 4, p. 38, pi. 3, figs. 24, 25. 
 
 ? bairdioides? Jones and Kirkby, 1884; Geol. Mag., decade 3, p. 358, pi. 12, 
 
 figs. 8 a-d. 
 
 ? elongata Jones and Kirkby, 1884; AnDals Mag. Nat. Hist., London, 6th series, 
 
 vol. 1, p. 361, pi. 12, fig. 10. Carboniferous. 
 
 ? elongata Jones and Kirkby, 1884; Geol. Mag., decade 3, p. 361, pi. 12, fig. 10. 
 
 fabulina Jones and Kirkby, 1879; Annals Mag. Nat. Hist., London, 5th series, 
 
 vol. 4, p. 31, pi. 2, figs. 1-9. 
 
 fabulina var. humilis Jones and Kirkby, 1879 ; Annals Mag. Nat. Hist., London, 
 
 5th series, vol. 4, p. 31, pi. 2, figs. 11-14. 
 
 fabulina Jones, 1889; Geol. Mag., decade 3, vol. 6, p. 270, figs. 1-4. 
 
 [ Cytherilla ] injlata Dawson, 1868; Acadian Geology, p. 206, fig. 48 b. 
 
 fabulina Jones and Kirkby, 1884; Geol. Mag., decade 3, vol. 1, p. 358, pi. 12, figs. 
 
 9 a-e. 
 
 Ceratiocaris McCoy, 1849; Annals Mag. Nat. Hist., London, vol. 4, p. 412. 
 
 aculeatus Hall, 1859; Pal. New York, vol. 3, p. 422"*, pi. 80 a, fig. 10. Waterlimo. 
 
 acuminatus Hall, 1859 ; Pal. New York, vol. 3, p. 422*, pi. 84, fig. 6. Waterlime. 
 
 acuminatus Pohlman, 1886 ; Bull. Buffalo Soc. Nat. Sci., vol. 5, p. 28, pi. 3, fig. 2. 
 
 annatus Hall. (See Echinocaris punctata.) 
 
 beecheri Clarke, 1881 ; Bull. U. S. Geol. Survey, No. 16, p. 44, pi. 2, fig. 1. 
 
 Devonian. 
 
 beecheri Hall, 1888; Pal. New York, vol. 7, p. 104, pi. 31, fig. 3. 
 
 [ Colpocaris ] bradleyi Meek, 1871 ; Proc. Acad. Nat. Sci. Phila., vol. 23, p. 332. 
 
 Lower Carboniferous. 
 
 [Onchus] deweyi Hall, 1852; Pal. New York, vol. 2, p. 320, pi. 71, figs. 1 a-d. 
 
 Niagara* 
 
 Bull. 63 11 
 
162 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [BULL. 63. 
 
 Ceratiocaris [ Colpocaris ] etytroides Meek, 1871; Proc. Acad. Nat. Sci. Phila., vol. 
 23, p. 334. Lower Carboniferous. 
 
 grandis Pohlman, 1881 ; Bull. Buffalo Soc. Nat. Sci., vol. 4, p. 19, fig. 5. 
 
 Waterlime. 
 
 longicaudus Hall, 1863; 16tli Rept. New York State Cab. Nat. Hist., p. 70, pi. 1, 
 
 fig. 7 ( not figs. 4, 5, 6). Hamilton. 
 
 longicaudus Packard, 1883 ; 12th Annual Rept. U. S. Geol. Survey Territories, 
 
 p. 450. 
 
 longicaudus Jones and Woodward, 1884; Geol. Mag., decade 3, vol. 1, p. 1. 
 
 longicaudus Etheridge, Woodward, and Jones; 3d Rept. Comm. Foss. Phyllo- 
 
 poda, p. 35. 
 
 longicaudus Hall, 1888; Pal. New York, vol. 7, p. 163, pi. 31, fig. 1. 
 
 Not C. longicaudus Clarke, 1885; Bull. U. S. Geol. Survey, No. 16, p. 20. 
 
 maccoyana Hall, 1859; Pal. New York, vol. 3, p. 421, pi. 84, figs. 1-5. 
 
 Waterlime. 
 
 f punctatus Hall. (See Echinocaris punctata.) 
 
 — — simplex Clarke, 1885 ; Bull. U. S. Geol. Survey, No. 16, p. 43, pi. 2, fig. 2. 
 
 Devonian. 
 
 — - ? simplex Hall, 1888; Pal. New York, vol. 7, p. 165, pi. 31, fig. 2. 
 
 ? sinuata Meek and Worthen, 1868; Am. Jour. Sci., 2d series, vol. 46, p. 22. 
 
 Coal Measures. 
 
 ? sinuata Meek and Worthen, 1868; Geol. Survey Illinois, vol. 3, p. 540, fig. a. 
 
 [ Solenocaris ] strigata, Meek, 1871; Proc. Acad. Nat. Sci. Phila., vol. 23, p. 335. 
 
 Lower Carboniferous. 
 
 [ Solenocaris ] strigata Meek, 1875 ; Pal. Ohio, vol. 2, p. 321, pi. 18, figs. 4 a-c. 
 
 The generic name of Solenocaris was used by Mr. J. Young for a genus of 
 the Paleozoic Crustacea in 1868. See Strigocaris. 
 
 Ciangopsis Salter, 1863; Name changed from Palceocrangon. 
 
 Cryptozoe Packard, 1886 ; Proc. Am. Philos. Soc., vol. 23, p. 381. 
 
 problematicus Packard, 1886 ; Proc. Am. Philos. Soc., vol. 23, p. 382, fig. 3, plate. 
 
 Carboniferous. 
 
 Cyclus De Koninck, 1841 ; M6m. Acad. Sci. Bruxelles, vol. 14, p. 18. 
 
 americana Packard, 1885 ; American Naturalist, vol. 19, p. 293. Coal Measures. 
 
 americana Packard, 1886; Mem. Nat. Acad. Sci., vol. 3, p. 143, pi. 5, figs. 1, 1 a; 
 
 pi. 6, figs. 4, 4 a. 
 
 Cythere Muller, 1785; Entomostraca, p. 64. 
 
 [ Beyrichia ] americana Shumard, 1858; TranB. Acad. Sci. St. Louis, vol. 1, p. 227. 
 
 Upper Coal Measures. 
 
 carbonaria Hall. (See Leperditia carbonaria.) 
 
 cincinnatiensis Meek. (See Entomis cincinnatiensis.) 
 
 crassimarginata Winchell, 1862 ; Proc. Acad. Nat. Sci. Phila., p. 429. Marshall. 
 
 irregularis Miller, 1878; Jour. Cincinnati Soc. Nat. Hist., vol. 1, p. 106, pi. 3,, 
 
 figs. 7, 7 a. Hudson.. 
 
 nebrascensis Geinitz, 1866 ; Carb. und Dyas in Nebraska, p. 2, pi. 1, fig. 2. 
 
 Coal Measures. 
 
 nebrascensis Meek, 1872 ; Rept. U. S. Geol. Survey Territories, Final Report 
 
 Nebraska, p. 237, pi. 11, figs. 1,2,3 a, b (?). 
 
 nebrascensis Keyes, 1888; Proc. Acad. Nat. Sci. Phila., p. 222. 
 
 ohiones Herrick, 1889; Bull. Den. Univ., vol. 4, p. 60, pi. 8, fig. 8; vol. 3, pi. 3, 
 
 fig. 19. Kinderhook. 
 
 ohiones Herrick, 1890 ; American Geologist, vol. 4, p. 254. 
 
 okeni. (See Leperditia okeni.) 
 
 simplex White and St. John, 1867 ; Prelim. Notice New Species Foss., p. 3. 
 
 St. Louis. 
 
 simplex White and St. John, 1868; Trans. Chicago Acad. Sci., vol, 1, p. 127. 
 
VOGDES.J 
 
 CATALOGUE OF NON-TRILOB1TES. 
 
 163 
 
 Carboniferous. 
 
 Cythere sp. ? Dawson, 1868 ; Acadian Geology, p. 256, fig. 78 a. 
 
 sublcevis. (See Leperditia sublaevis. ) 
 
 subrecta. (See Leperditia subrecta.) 
 
 Cytherina Lamarck, 1818; Animaux sans Vert., vol. 5, p. 125. 
 
 alia. (See Leperditia alta.) 
 
 crenulata Emmons, 1855 ; Am. Geology, vol. 1, p. 221, figs. 75 a-d. Trenton. 
 
 cylindrica. (See Isochilina cylindrica.) 
 
 emmonsi Vogdes, 1889 ; Annals N. Y. Acad. Sci., vol. 5, p. 13, to replace C. sub- 
 
 cylindrica. 
 
 spinosa. (See Beyrichia spinosa.) 
 
 subcylindrica Emmons, 1855; Am. Geology, vol. 1, p. 220, fig. 75 b. Trenton. 
 
 This name was used by Munster for a species of this genus. Change to C. 
 emmonsi. 
 
 subelliptica Emmons, 1855; Am. Geology, vol. 1, p. 220, figs. 75 a. 
 
 Trenton. 
 
 Cytherellina Jones and Holl, 1869 ; Annals Mag. Nat. Hist., London, 4th series, vol. 
 3, p. 215. 
 
 grandella Whitfield, 1882 ; Bull. Am. Mus. Nat. Hist. New York, vol. 1, p. 94, 
 
 pi. 9, figs. 28, 29. Warsaw. 
 
 Cytheropsia McCoy, 1855 ; Synopsis Classification Brit. Pal. Rocks, pi. 1 L., fig. 2. 
 No definite descriptign of the genus given. 
 
 concinna Jones. (See Primitia concinna.) 
 
 rugosa Jones. (See Primitia rugosa.) 
 
 silique Jones, 1858 ; Annals Mag. Nat. Hist., 3d series, London, vol. 1, p. 249, 
 
 pi. 10, fig. 6. Trenton. 
 
 silique Jones, 1858 ; Geol. Survey Canada, decade 3, p. 99. 
 
 silique Jones, 1869 ; Annals Mag. Nat. Hist., London, 4th series, vol. 3, p. 216, 
 
 pi. 14, figs. 1-6. 
 
 Dipeltis Packard, 1885; Am. Naturalist, vol. 19, p. 293. 
 
 diplodiscus Packard, 1885; Am. Naturalist, vol. 19, p. 293. Carboniferous. 
 
 diplodiscus Packard, 1886; Mem. Nat. Acad. Sci., vol. 3, p. 145, pi. 5, figs. 2,2 a. 
 
 Diplostylus Salter, 1863 ; Quart. Jour. Geol. Soc. London, vol. 19, p. 76. 
 
 dawsoni Salter, 1863 ; Quart. Jour. Geol. Soc. London, vol. 19, p. 77, fig. 6. 
 
 Coal Measures. 
 
 Dipterocaris Clarke, 1883 ; Am. Jour. Sci., 3d series, vol. 25, p. 121. 
 
 pennae-daedali Clarke, 1883 ; Am. Jour. Sci., 3d series, vol. 25, p. 122, fig. 1. 
 
 Chemung. 
 
 pennae-daedali Jones and Woodward, 1884 ; Geol. Mag., decade 3, vol. 1, p. 349. 
 
 pennae-daedali Etheridge, Woodward, and Jones, 1884 ; 2d Kept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 11. 
 
 pennae-daedali Etheridge, Woodward, and Jones, 1885 ; 3d Rept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 3. 
 
 pennae-daedali Hall, 1888 ; Pal. New York, vol. 7, p. 200, pi. 35, fig. 24. 
 
 pennae-daedali Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 9. 
 
 percervae Clarke, 1883 ; Am. Jour. Sci., 3d series, vol. 25, p. 123, figs. 4,5. 
 
 Chemung. 
 
 percervae Jones and Woodward, 1884 ; Geol. Mag., decade 3, vol. 1, p. 349. 
 
 percervae Etheridge, Woodward, and Jones, 1884 ; 2d Rept. Comm. Foss. Phyllo- 
 
 lopoda Pal. Rocks, p. 11. 
 
 percervae Etheridge, Woodward, and Jones, 1885 ; 3d Rept. Comm. Foss. Pbyllo- 
 
 poda Pal. Rocks, p. 3. 
 
 percervae Hall, 1888 ; Pal. New York, vol. 7, p. 202, pi. 35, figs. 20, 21. 
 
 percervae Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm, Foss, Phyllo- 
 poda Pal. Rocks, p. 9. 
 
164 
 
 [BULL. 63 . 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Dipterocaris prcene Clarke, 1883 ; Am. Jour. Sci., 3d series, vol. 25, p. 122, figs. 2, 3. 
 
 Chemung. 
 
 prcene Jones and Woodward, 1884; Geol. Mag., decade 3, vol. 1, p. 349. 
 
 prcene Etheridge, Woodward, and Jones, 1884 ; 2d Rept. Comm. Foss. Phyllo- 
 
 poda Pal. Rocks, p. 11. 
 
 prcene Etheridge, Woodward, and Jones, 1885 ; 3d Rept. Comm. Foss. Phyllo- 
 
 poda Pal. Rocks, p. 3. 
 
 prcene Hall, 1888 ; Pal. New York, vol. 7, p. 201, pi. 35, figs. 25-27. 
 
 prcene Etheridge, Woodward, and Jones, 1888 ; 6th Rept. Comm. Foss. Phyllo- 
 
 pod a Pal. Rocks, p. 9. 
 
 Dithyrocaris (Scouler, 1843, MS.) Portlock, 1843; Rept. Geol. Londonderry, etc., p. 
 313. 
 
 belli Woodward, 1870; Geol. Mag.,. decade 2, vol. 8, p. 106, pi. 3, figures. 
 
 Devonian. 
 
 belli Etheridge, Woodward, and Jones, 1887 ; 5th Rept. Comm. Foss. Phyllo- 
 
 poda Pal. Rocks, p. 6. 
 
 belli Hall, 1888 ; Pal. New York, vol. 7, p. 194. 
 
 carbonaria Meek and Worthen, 1870 ; Proc. Acad. Nat. Sci. Phila., vol. 22, p. 55. 
 
 Coal Measures. 
 
 carbonaria Meek and Worthen, 1873 ; Geol. Survey Illinois, vol. 5, p. 6! 8, pi. 
 
 32, fig. 1. 
 
 carbonaria White, 1884 ; 13th Rept. Dept. Geol. Nat. Hist. Indiana, p. 178, pi. 
 
 39, fig. 2. 
 
 neptuni Hall. (See Mesothyra neptuni.) 
 
 DolichocepliaJa Claypole,*1883 ; Proc. Am. Philos. Soc., vol. 21, p. 236. 
 
 locoanci idem ; p.236, plate. (See Stylonurus excelsior.) 
 
 Dolichopterus (subgenus Eurypterus) Hall, 1859; Pal. New York, vol. 3, p. 414. * 
 
 macrocheous Hall, 1859 ; Pal. New York, vol. 3, p. 414,* pi. 83, fig. 1 ; pi. 83 a, fig. 1. 
 
 Waterlime. 
 
 Echinocaris Whitfield, 1880 ; Am. Jour. Sci., 3d series, vol. 19, p. 34. 
 
 condylepsis Hall, 1888 ; Pal. New York, vol. 7, p. 173, pi. 19, figs. 14-17. 
 
 Chemung. 
 
 multinodosa Whitfield, 1880 ; Am. Jour. Sci. , 3d series, vol. 19, p. 38, fig. 8. (Plates 
 
 with author’s special edition only.) Erie Shales. 
 
 multinodosa Packard, 1882 ; Am, Naturalist, vol. 16, p. 952, fig. 10. 
 
 multinodosa Packard, 1883 ; 12th Rept. U. S. Geol. Survey Territories, p. 451, 
 
 fig. 71 a. 
 
 multinodosa Beecher, 1884 ; 2d Geol. Survey Penn., vol. PPP, p. 5. 
 
 multinodosa Etheridge, Woodward, and Jones, 1885 ; 3d Rept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 35. 
 
 multinodosa Hall, 1888 ; Pal. New York, vol. 7, p. 180, pi. 29, figs. 18-19. 
 
 multinodosa Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 8. 
 
 [ Ceratiocaris] punctatus Hall, 1863; 16th Rept. New York State Cab. Nat. Hist. 
 
 p. 74, pi. 1, fig. 8. Hamilton. 
 
 punctatus Whitfield, 1880; Am. Jour. Sci., 3d series, vol. 19, p. 39. 
 
 Syn., Ceratiocaris armatus Hall, 1863; 16th Rept. New York State Cab. Nat. 
 Hist., p. 72, pi. 1, figs. 1-3. 
 
 Ceratiocaris armatus Hall, 1876; Illus. Devonian Foss., pi. 23, figs. 4,5. 
 
 [ Ceratiocaris ( Aristozoe)] punctatus Hall, 1876; Illus. Devonian Foss.,.Expl. 
 
 pi. 23, fig. 7. 
 
 punctatus Packard, 1882; Am. Naturalist, vol. 16, p.952, fig. 12. 
 
 punctatus Packard, 1883 ; 12th Rept. U. S. Geol. Survey Territories, p. 450,. 
 
 fig. 70. 
 
 Syn., armatus Packard, 1883 ; 12th Rept. U. S. Geol. Survey Terri tories^p. 451. 
 
vogdes.] CATALOGUE OF NON-TRILOBITES. 165 
 
 Echinocaris punctatus Beecher, 1884 ; 2d Geol. Survey Penn.,voI. PPP, p. 6, pi. 1, 
 figs. 13-16 ; also fig. 1 in text, page 4. 
 
 Syn., armatus Jones and Woodward, 1884; Geol. Mag., decade 3, vol. 1, p. 2, pi. 
 
 13, fig. 2. 
 
 armatus Etheridge, Woodward, and Jones, 1885; 3d Rept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 35. 
 
 punctatus Hall, 1888; Pal. New York, vol. 7, p. 166, pi. 27, fig. 10 ; pi. 28, fig. 1-7 ; 
 
 ' pi. 29, fig. 1-8. 
 
 punctatus Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 8. 
 
 .pustulosa Whitfield, 1880 ; Am. Jour. Sci., 3d series, vol. 19, p. 38, pi. fig. 7 
 
 (plate with author’s special edition only). Erie Shales. 
 
 pustulosa Packard, 1883 ; 12th Rept. U. S. Geol. Survey Territories, p. 451. 
 
 pustulosa Beecher, 1884 ; 2d Geol. Survey Penn., vol. PPP., p. 5. 
 
 pustulosa Jones and Woodward, 1884 ; Geol. Mag., decade 3, vol. 1, p. 2, pi. 13, 
 
 fig. 6. 
 
 pustulosa Etheridge, Woodward, and Jones, 1885; 3d Rept. Comm. Foss- 
 
 Phyllopoda Pal. Rocks, p. 35. 
 
 pustulosa Hall, 1888 ; Pal. New York, vol. 7, p. 178, pi. 29, figs. 9, 10. 
 
 pustulosa Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 8. 
 
 socialis Beecher, 1884 ; 2d Geol. Survey Penn., vol. PPP, p. 10, pi. 1, figs. 1- 
 
 le. Chemung. 
 
 socialis Etheridge, Woodward, and Jones, 1885 ; 3d Rept. Comm. Foss. Phvllo. 
 
 poda Pal. Rocks, p. 35. 
 
 socialis Hall, 1888 ; Pal. New York, vol. 7, p. 174, pi. 30, figs. 1-12. 
 
 socialis Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. Phyllo- 
 poda Pal. Rocks, p. 8. 
 
 sublevis Whitfield, 1880 ; Am. Jour. Sci., 3d series, vol. 19, p. 36, pi. figs. 4-6 
 
 (plate with the authors special edition only). Erie Shales. 
 
 sublevis Packard, 1882; Am. Naturalist, vol. 16, p. 952, fig. 11. 
 
 sublaevis Packard, 1883; 12th Rept. U. S. Geol. Survey Territories, p. 450, fig. 
 
 71 b. 
 
 sublevis Beecher, 1884; 2d Geol. Survey Penn., vol. PPP, p. 5. 
 
 sublaevis Jones and Woodward, 1884 ; Geol. Mag., decade 3, vol. 1. p. 2, pi. 13, figs. 
 
 3, 4, 5. 
 
 sublaevis Etheridge, Woodward, and Jones, 1885; 3d Rept. Comm. Foss. Phyllo- 
 poda Pal. Rocks, p. 35. 
 
 sublaevis Hall, 1888; Pal. New York, vol. 7, p. 176, pi. 29, figs. 11-13. 
 
 sublaevis Etheridge, Woodward, and Jones, 1888 ; 6th Rept. Comm. Foss. Phyl- 
 lopoda Pal. Rocks, p. 8. 
 
 whitfieldi Clarke, 1885 ; Bull. U. S. Geol. Survey, No. 16, p. 45, pi. 2, figs. 3, 4. 
 
 Portage. 
 
 whitfieldi Hall, 1888; Pal. New York, vol. 7, p. 172, pi. 29, figs. 20, 21. 
 
 whitfieldi Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. Phyl- 
 lopoda Pal. Rocks, p. 8. 
 
 Echinognathus Walcott, 1882; Am. Jour. Sci., 3d series, vol. 23, p. 213. 
 
 clevelandi Walcott, 1882 ; Am. Jour. Sci., 3d series, vol. 23, p. 213, figs. 1, 2. 
 
 Utica. 
 
 [ Eurypterus ?] clevelandi Walcott, 1882; Am. Jour. Sci., 3d series, vol. 23, p. 151. 
 
 Elymocaris Beecher, 1884; 2d Geol. Survey Penu., vol. PPP, p. 13. 
 
 siliqua Beecher, 1884 ; 2d Geol. Survey Penn., vol. PPP, p. 13, pi. 2, figs. 1, 2. 
 
 Chemung. 
 
 siliqua Etheridge, Woodward, and Jones, 1885; 3d Rept. Comm. Foss. Phyllo- 
 poda Pal. Rocks, p. 35. 
 
166 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. [bull.63. 
 
 Elymocaris siliqua Hall, 1888; Pal. New York, vol. 7, p. 182, pi. 31, figs. 5, 6. 
 
 siliqua Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. Phyllo- 
 
 poda Pal. Rocks, p. 8. 
 
 Entomis Jones, 1861 ; Mem. Geol. Survey Scotland, Expl. Map 32, p. 137 ; also, An- 
 nals Mag. Nat. Hist., London, 4th series, vol. 11, p. 413. 
 
 [ Cythere ] cincinnatiensis Meek, 1871 ; Proc. Acad. Nat. Sci. Phila., vol. 23, p. 331. 
 
 Hudson. 
 
 [Cythere ] cincinnatiensis Meek, 1873; Pal. Ohio, vol. 1, p. 158, pi. 14, figs. 1 a- 
 
 1 d. 
 
 [ Cythere ] cincinnatiensis Miller, 1874; Cincinnati Quart. Jour. Sci., vol. 1, p. 
 
 120 . 
 
 cincinnatiensis Jones, 1884; Annals. Mag. Nat. Hist., London, 5th series, vol. 
 
 14, note p. 395. 
 
 rhomboidea Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 10, pi. 2, figs. 9, 10 a, b. 
 
 Hamilton. 
 
 Equisetides wrightiana. This species is referred by Woodward and Jones (3d Report 
 Comm. Foss. Phyllopoda Brit. Assoc., 1885, p. 360) to Echinocaris. Prof. James 
 Hall places it provisionally with Stylonurus, which see. 
 
 Estheria Ruffell, 1857 ; Mus. Senckenberg, vol. 2, p. 119. 
 
 dawsoni Jones, 1870; Geol. Mag., vol. 7, p. 220, pi. 9, fig. 15. Carboniferous. 
 
 dawsoni Jones, 1878; Geol. Mag., decade 2, vol. 2, p. 101, pi. 3, fig. 2. 
 
 sp. ? Dawson, 1868 ; Acadian Geology, p. 256, fig. 78 d. 
 
 dawsoni Jones and Kirkby, 1884 ; Geol. Mag., decade. 3, voi. 1, p. 361, pi. 12, fig. 12. 
 
 pulex Clarke, 1882; Am. Jour. Sci., 3d series, vol. 23, p. 476, pi., fig. 4. 
 
 Hamilton. 
 
 pulex Packard, 1883 ; 12th Rept. U. S. Geol, Survey Territories, p. 355. 
 
 pulex Etheridge, Woodward, and Jones, 1885; 5th Rept. Comm. Foss. Phyllo- 
 poda Pal. Rocks, p. 10. 
 
 pulex Hall, 1888; Pal. New York, vol. 7, p. 206, pi. 35, figs. 10, 11. 
 
 pulex Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. Phyllo- 
 poda Pal. Rocks, p. 9. 
 
 Euproops Meek, 1867 ; Am. Jour. Sci., 2d series, vol. 34, p. 394. (See Bellinurus and 
 Frestwichia.) 
 
 Eurychilinda Ulrich, 1889; Contributions Micro-Palseont., pt. 2, p. 52. 
 
 mantiobensis Ulrich, 1889; Contributions Micro-Palseont., pt. 2, p. 53, pi. 9, 
 
 figs. 10, 10 a. Hudson. 
 
 reticulata Ulrich, 1889; Contributions Micro-Palseont., pt. 2, p. 52, pi. 9, figs. 
 
 9, 9 a. Trenton. 
 
 striato-marginata (Miller) Ulrich, 1889; Contributions Micro-Palseont., pt. 2, 
 
 p. 52. 
 
 For other references, see Beyrichia striato-marginata. 
 
 Eurypterus De Kay, 1825; Annals Lyceum Nat. Hist. N. Y., vol. 1, pt. 2, p. 375. 
 
 beecheri Hall, 1884 ; 2d Geol. Survey Pennsylvania, vol. PPP, p. 30, pi. 3, fig. 1. 
 
 Chemung. 
 
 beecheri Hall, 1888 ; Pal. New York, vol. 7, p. 156, pi. 27, fig. 5. 
 
 beecheri Etheridge, Woodward, and Jones, 1888 ; 6th Rept. Comm. Fossil Phyllo- 
 poda Pal. Rocks, p. 9. 
 
 boylei Whiteaves, 1884 ; Pal. Fossils, vol. 3, pt. 1, p. 42, pi. 7, fig. 3. Guelph. 
 
 dekayi Hall, 1859 ; Pal. New York, vol. 3, p. 411*, pi. 82, fig. 1. Waterlime. 
 
 eriensis Whitfield, 1881 ; Annals New York Acad. Sci., vol. 2, p. 196. 
 
 Lower Helderberg. 
 
 giganteus Pohlman, 1882; Bull. Buffalo Soc. Nat. Sci., vol. 4, p. 41, pi. 2, fig. 1. 
 
 Waterlime. 
 
 lacustriB Harlan, 1834; Trans. Geol. Soc. Pennsylvania, vol. l,p. 98, pi. 5, fig. 2. 
 
 Waterlime. 
 
V0GDE8. J 
 
 CATALOGUE OF NON-TRILOBITES. 
 
 167 
 
 Eurypterus lacustris Harlan, 1835 ; Med. Phys. Researches, p. 297, plate, fig. 2. 
 
 lacustris Hall, 1859; Pal. New York, vol. 3, p. 407*, pi. 81, figs. 1-11; pi. 81 a, 
 
 fig. 1 ; pi. 81 b, figs. 1-5 ; pi. 83 b, fig. 3 ; also fig. 5 in text p. 400*. 
 
 lacustris var. robustus Hall, 1859 ; Pal. New York, vol. 3, p. 410*, pi. 81 c, fig. 2. 
 
 [ Dolichopterus ] mansfieldi Hall, C. E.,1877; Proc. Am. Philos. Soc., vol. 16, 
 
 p. 621. Carboniferons. 
 
 mansfieldi Hall, 1884 ; 2d Geol. Survey Pennsylvania, vol. PPP, p. 32, pi. 4, 
 
 figs. 1-8; pi. 5, figs. 1-11 ; pi. 6, fig. 1 ; pi. 7, fig. 1 ; pi. 8, figs. 1-3. 
 
 [ Anthraconectes ] mazonensis Meek and Worthen, 1868; Am. Jour. Sci., 2d 
 
 series, vol. 46, p. 21. Coal Measures. 
 
 [ Anthraconectes ] mazonensis Meek and Worthen, 1868 ; Geol. Survey Illinois, 
 
 vol. 3, p. 544, figures. 
 
 — — [Anthraconectes'] mazonensis Hall, 1884; 2d Geol. Survey Pennsylvania, vol. 
 PPP, p. 25, fig. 2; p. 27, fig. 3. 
 
 [ Anthraconectes ] mazonensis White, 1884 ; 13th Ann. Rept. Dept. Geol. Nat. 
 
 Hist. Indiana, p. 168, pi. 37, figs. 1, 2, 3. 
 
 microphthalmus Hall, 1859; Pal. New York, vol. 3, p. 407*, pi. 80 a, fig. 7. 
 
 Lower Helderberg. 
 
 pachycheirus Hall, 1859 ; Pal. New York, vol. 3, p. 412*, pi. 8, figs. 1-3. 
 
 Waterlime. 
 
 pennsylvanicus Hall, C. E., 1877 ; Trans. Am. Philos. Soc. Phila., vol. 7, p. 621. 
 
 Carboniferous. 
 
 pennsylvanicus Hall, 1884 ; 2d Geol. Survey Pennsylvania, vol. PPP, p. 31, 
 
 pi. 5, fig. 18. 
 
 pohlmani Vogdes, 1889 ; to take the place of the preoccupied name of E. scor- 
 
 piovis Grote and Pitt. Ann. N. Y. Acad. Sci., vol. 5, No. 1. 
 
 potens Hall, 1884 ; 2d Geol. Survey Pennsylvania, vol. PPP, pi. 4, figs. 9, 10. 
 
 Carboniferous. 
 
 prominens Hall, 1884 ; Proc. Am. Assoc. Adv. Sci., vol. 33, p. 420. Clinton. 
 
 prominens Hall, 1888; Pal. New York, vol. 7, p. 157, pi. 27, figs. 3, 4. 
 
 pulicaris Salter, 1863; Quart. Jour. Geol. Soc. London, vol. 19, p. 78, figs. 9, 10. 
 
 Coal Measures. 
 
 pulicaris Dawson, 1868 ; Acadian Geology, p. 523, figs. 179 a, b. 
 
 pustulosus Hall, 1859 ; Pal. New York, vol. 3, p. 413*, pi. 83 b, fig. 1. 
 
 Waterlime. 
 
 remipes De Kay. Waterlime. 
 
 Syn., Fossil Fish Mitchell, 1818; Am. Monthly Mag., vol. 3, p. 291. 
 
 remipes De Kay, 1825; Annals Lyceum Nat. Hist., vol. 1, p. 375, pi. 29. 
 
 remipes Harlan, 1834 ; Trans. Geol. Soc. Penn., vol. 1, p. 96, pi. 5. 
 
 remipes Harlan, 1835; Medical Phys. Researches, p. 297, pi., fig. 1. 
 
 remipes Milne-Ed wards, 1840; Hist. Nat. Crust., vol. 3, p. 422. 
 
 remipes Burmeister, 1843; Org. Trilobiten, p. 62 (Ray Soc. ed., p. 54). 
 
 remipes Bronn, 1837 ; Lethea Geognostica, vol. 1, p. 666, pi. 9 s , fig. 1 ; pi. 9, fig. 1. 
 
 remipes Salter, 1859 ; Quart. Jour. Geol. Soc. London, vol. 15, p. 255. 
 
 remipes Nieszkowski, 1858; Der Eurypterus remipes, etc., pis. 1, 2, 3. 
 
 remipes Hall, 1859 ; Pal. New York, vol. 3, p. 404, pi. 80, figs. 1-12 ; pi. 80 a, 
 
 figs. 1-6; pi. 83 b, fig. 2, also p. 403*, figs. 6, 7. 
 
 remipes (numerous authors). 
 
 [Eusarcus] grandis Grote and Pitt, 1875 ; Bull. Buffalo Soc. Nat. Sci., vol. 3, p. 17. 
 
 Waterlime. 
 
 Referred by J. Pohlman (Bull. Buffalo Soc. Nat. Sci., vol. 5, p. 31) to 
 Eurypterus scorpionia. An almost similar terra, E. scorpioides was used for a 
 species of this genus by H. Woodward in 1868; I suggest that of E. pohlmani 
 for this species. 
 
 [ Eu8arcu8~\ scorpionis Grote and Pitt, 1875; Bull. Buffalo Soc. Nat. Sci., vol. 3, 
 
 pp. 1, 17, photographic plate. Waterlime. 
 
168 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 (BULL. 63 . 
 
 Eurypterus [ Eusarcus ] scorpionis (Grote and Pitt) Pohlman, 1886; Bull. Buffalo 
 Soc. Nat. Sci., vol. 5, p. 30, pi. 2, fig. 3. 
 
 [ Eusarcus ] grandis (Grote and Pitt) Pohlman, 1886; Bull. Buffalo Soc. Nat. Sci., 
 
 vol. 5, p. 31. 
 
 Referred to Eurypterus pohlmani Vogdes, 1889; Annals N. Y. Acad. Sci., vol. 5, 
 
 p. 22. 
 
 Hymenocaris Salter, 1853 ; 22dRept. Brit. Assoc. Adv. Sci., Trans, of sec., p. 56. 
 Isochilina Jones, 1857 ; Mem. Geol. Survey Canada, decade 3, p. 97. 
 
 ^Leperditia ( Isochilina )] armata Walcott, 1883; Des. New Sp. Foss. Trenton 
 
 Group, p. 7. 
 
 \_Leperditia ( Isochilina )] armata Walcott, 1884 ; 35th Rept. N. Y. State Mus. Nat. 
 
 Hist., p. 213. 
 
 cristata (Whitfield) Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 23, pi.. 1, 
 
 fig. 8. Calciferous. 
 
 For other references, see Primitia cristata. 
 
 [ Cyilierina ] cylindrica Hall, 1852; Pal. New York, vol. 2, p. 14, pi. 4, figs. 8 a, b. 
 
 Medina. 
 
 Prof. T. Rupert Jones (Quart. Jour. Geol. Soc., vol. 46, 1890, p. 8) refers this 
 
 species to Leperditia cylindrica. 
 
 \_Leperditia ( Isochilina )] cylindrica Jones, 1858; Annals Mag. Nat. Hist., 3d 
 
 series, vol. 1, p. 253 ; also, Geol. Survey Canada, decade 3, p. 101. 
 
 [ Leperditia ( Isochilina )] cylindrica Hall, 1871 ; Description n. sp. Fossils Hud- 
 son River Group. 
 
 [ Leperditia ( Isochilina )] cylindrica Hall, 1872; 24th Rept. N. Y. State Mus. Nat. 
 
 Hist., p. 231, pi. 8, $g. 2; also, Pal. Ohio, vol. 2, 1875, p. 101, pi. 4, fig. 5. 
 
 Prof. T. Rupert Jones (Quart. Jour. Geol. Soc., vol. 46, 1890, p. 8) refers this 
 species to Primitia minuta Eichwald. 
 
 cylindrica Miller, 1875 ; Cincinnati Quart. Jour. Sci., vol. 2, p. 351. 
 
 fabacea Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 22, pi. 2, fig. 11. 
 
 Hamilton. 
 
 [ Leperditia ( Isochilina )] gracilis Jones, 1858; Annals Mag. Nat. Hist., London, 
 
 3d series, vol. 1, p. 248, pi. 10, fig. 2; also, Geol. Survey Canada, decade 3, p. 98, 
 pL 2, fig. 15. Trenton. 
 
 gregaria (Whitfield) Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 22, pi. 1, figs. 
 
 9, 10. 
 
 For other references, see Primitia gregaria. 
 
 jonesi Wetherby, 1881 ; Jour. Cincinnati Soc. Nat. Hist., vol. 4, p. 80, pi. 2, figs. 
 
 7, 7 a. Subcarboniferous. 
 
 lineata Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 21, pi. 2, figs. 5 a, b, 8 a, b. 
 
 Hamilton. 
 
 [ Leperditia ( Isochilina )] minutissima Hall, 1871 ; Des. New Species Foss. Hud- 
 son River Group, p. 7. 
 
 [ Leperditia ( Isochilina )] minutissima Hall, 1872; 24th Rept. New York State 
 
 Mus. Nat. Hist., p. 231, pi. 8, fig. 13. 
 
 [ Leperditia ( Isochilina )] minutissima Hall and Whitfield, 1875 ; Pal. Ohio, vol. 
 
 2, p. 102, pi. 4, fig. 5. (See Aparchites minutissima.) 
 
 [ Leperditia ( Isochilina )] Ottawa Jones, 1858; Annals Mag. Nat. Hist., London, 
 
 3d series, vol. 1, p. 248, pi. 11, fig. 1. Chazy. 
 
 [ Leperditia ( Isochilina )] Ottawa Jones, 1858 ; Geol. Survey Canada, decade 3, p. 
 
 97, pi. 9, fig. 14. 
 
 Ottawa Jones, 1884 ; Annals Mag. Nat. Hist., London, 5th series, vol. 14, p. 345. 
 
 seelyi (Whitfield) Jones, 1890 ; Quait. Jour. Geol. Soc., vol. 46, p. 22, pi. 1, fig. 7. 
 
 For other references, see Primitia seelyi. 
 
 Klcedenia Jones and Holl, 1886; Annals Mag. Nat. Hist., London, 5th series, vol. 17, 
 p. 362. 
 
V0GDES.] 
 
 CATALOGUE OF NON-TRILOBITES. 
 
 169 
 
 Klcedenia [Be-yrichia] notata Hall, 1859 ; Pal. New York, vol. 3, p. 379, pi. 79 b, figs. 
 3 a, b, c. Lower Helderberg. 
 
 [ Beyrichia ] notata var. ventricosa Hall, 1859 ; idem, p. 380, pi. 79 b, figs. 4 a, b, c. 
 
 notata Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 13, pi. 4, figs. 22, 23. 
 
 notata var. ventricosa Jones, 1890 ; Quart. J6ur. Geol. Soc., vol. 46, p. 14, pi. 1, 
 
 figs. 1 a, b; pi. 4, fig. 24. 
 
 pennsylvanica Jones, 1889; American Geologist, vol. 4, p. 341, pi., figs. 5-9. 
 
 Lower Helderberg. 
 
 simplex Jones, 1889 ; American Geologist, vol. 4, p. 338, pi., fig. 14. 
 
 Upper Devonian. 
 
 Leaia Jones, 1862 ; Mon. Fossil Estheriae, p. 115. 
 
 [ Cypricardia ] leidyi Lea, 1855; Proc. Acad. Nat. Sci. Phila., vol. 7, p. 341, pi. 4. 
 
 Coal Measures. 
 
 leidyi Jones, 1862; Mon. Fossil Estheriae, p. 116, pi. 5, figs. 11, 12. 
 
 leidyi Dawson, 1868 ; Acadian Geology, p. 256, fig. 78 c. 
 
 leidyi Packard, 1882; 12th Rept. U. S. Geol. Survey Territories, p. 358, fig. 24. 
 
 leidyi Jones, 1870; Geol. Mag., vol. 7, p. 219, pi. 9, fig. 11; also, Geol. Mag., 
 
 decade 3, vol. 1, p. 361, pi. 12, fig. 13. 
 
 tricarinata Meek and Worthen, 1868; Geol. Survey Illinois, vol. 3, p. 541, figs. 
 
 Bi, B 2 , B :{ . Coal Measures. 
 
 tricarinata White, 1884 ; 13th Ann. Rept. Dept. Geol. Nat. Hist. Indiana, p. 167, 
 
 pi. 39, figs. 10-13. 
 
 Leperditia Rouault, 1851 ; Bull. Soc. G6ol. France, 2d series, vol. 8, p. 377. 
 
 [ Cytherina ] alta Conrad, 1842; Geol. Rept. New York, 3d Geol. Dist. (Vanuxem), 
 
 p. 112. Lower Helderberg. 
 
 [ Cytherina ] alta ? Hall, 1852 ; Pal. New York, vol. 2, p. 338, pi. 78, figs. 2 a-d. 
 
 Referred to Leperditia jonesi Hall, idem, vol. 3, p. 372. 
 
 alta Jodos, 1856 ; Annals and Mag. Nat. Hist., London, 2d series, vol. 17, p. 88, pi. 
 
 7, figs. 6, 7. 
 
 alta Jones, 1858 ; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 250, pi. 10, 
 
 figs. 10, 11. 
 
 alta Hall, 1859; Pal. New York, vol. 3, p. 373, pi. 79 a, figs. 6 a-e. 
 
 alta Meek, 1873 ; Pal. Ohio, vol. 1, p. 187, pi. 17, figs. 2 a, b. 
 
 alta Jones, 1881'; Annals Mag. Nat. Hist., London, 5th series, vol. 8, p. 346. 
 
 alta Whitfield, 1882 ; Geol. Wisconsin, vol. 4, p. 323, pi. 25, figs. 8, 9. 
 
 alta Jones, 1884 ; Annals Mag. Nat. Hist., London, 5th series, vol. 14, p. 343. 
 
 alta Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 25, pi. 1, figs. 6 a, b. 
 
 amygdalina Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 
 
 341. Trenton. 
 
 amygdalina Jones, 1858 ; Geol. Survey Canada, decade 3, p. 97, pi. 11, figs. 18, 19. 
 
 amygdalina Jones, 1881; Annals Mag. Nat. Hist., London, 5th series, vol. 8, p. 
 
 344, pi. 19, fig. 9. 
 
 amygdalina Jones, 1884 ; Annals Mag. Nat. Hist., London, 5th series, vol. 14, p. 
 
 342. 
 
 angulifera Whitfield, 1881 ; Annals New York Acad. Sci., vol. 2, p. 199. 
 
 Lower Helderberg. 
 
 anna Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 347, pi. 
 
 9, fig. 8. Calciferous. 
 
 anna Jones, 1858; Geol. Survey Canada, decade 3, p. 96, pi. 11, fig. 13. 
 
 anticostiana Jones, 1884 ; Annals Mag. Nat. Hist., London, 3d series, vol. 14, p. 
 
 241. Hudson. 
 
 Syn., canadenns var. anticostiana J ones, 1858; Annals Mag. Nat. Hist., London, 
 3d series, vol. 1, p. 341. Hudson. 
 
 canadensis var. anticostiana Jones, 1858 ; Geol. Survey Canada, decade 3, p. 
 95, pi. 11, fig. 17. 
 
170 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 [bull. 63. 
 
 Leperditia anticostiana Billings, 1866; Catalogue Sil. Foss., Anticosti, p. 68. 
 
 Syn., fabulUes (Conrad) var. anticostiana Jones, 1881; Annals Mag. Nat. Hist., 
 London, 5th series, vol. 8, p. 344, pi. 19, fig. 8. 
 
 arctica Jones, 1856; Annals Mag. Nat. Hist., London, 2d series, vol. 17, p. 87, 
 
 figs. 1-5. Upper Silurian. 
 
 Syn., balthica var. arctica (Jones) Salter, 1852; Appendix Sutherland’s Jour. Voy- 
 age Baffin's Bay, vol. 2, p. ccxxi, pi. 5, fig. 13. 
 balthica var. arctica (Jones) Salter, 1853; Quart. Jour. Geol. Soc. London, 
 vol. 9, p. 314. 
 
 argenta Walcott, 1886; Bull. U. S. Geol. Survey, No. 30, p. 146, pi. 8, fig. 5. 
 
 Middle Cambrian. 
 
 billingsi Jones, 1856; Annals Mag. Nat. Hist., London, 2d series, vol. 8, p. 345, 
 
 pi. 15, fig. 9. Trenton. 
 
 bivertex Ulrich, 1879; Jour. Cincinnati Soc. Nat. Hist., vol. 2, p. 11, pi. 7, figs. 
 
 5,5 a. Hudson. 
 
 bivia White, 1874 ; Kept. Invert. Foss. U. S. Geog. and Geol. Survey W. 100th 
 
 Mer., p. 11. Quebec. 
 
 bivia White, 1877; U. S. Geog. and Geol. Survey W. 100th Mer., Palseont., vol. 
 
 4, p. 58, pi. 3, figs. 7 a-d. 
 
 byrnesi Miller, 1874 ; Cincinnati Quart. Jour. Sci., vol. 1, p. 123, fig. 10. (See 
 
 .SJchmina beyrnesi.) Hudson. 
 
 caecigena Miller, 1881; Jour. Cincinnati Soc. Nat. Hist., vol. 1, p. 263, pi. 6, 
 
 figs. 5, 5 a. Hudson. 
 
 canadensis Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 
 
 244, pi. 9, figs. ll-li>. Chazy and Trenton. 
 
 canadensis Jones, 1858 ; Geol. Survey Canada, decade 3, p. 92 ; var. nana, pi. 11, 
 
 figs. 6,7,9,10, and labrosa, pi. 11, fig. 8. 
 
 canadensis Jones, 1881 ; Annals Mag. Nat. Hist., London, 5th series, vol. 14, p. 
 
 340. 
 
 Compare Leperditia turgida, L. concinnula, and L. ventralis. 
 
 canadensis var. pauquettiana Jones. (See Leperditia louckana.) 
 
 [Cy there] carbonaria Hall, 1858; Trans. Albany Inst., vol. 4, p. 33. Warsaw. 
 
 carbonaria Whitfield, 1882; Bull. Am. Mus. Nat. Hist., New York, vol. 1, p. 94, 
 
 pi. 9, figs. 24-27. 
 
 capax Safford ; Geol. Tennessee. (Not defined. ) 
 
 cayuga Hall, 1861 ; Des. New Species Foss., p. 83. Corniferous. 
 
 cayuga Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 111. 
 
 claypolei Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 25, pi. 3, figs. 17 a-c. 
 
 Cincinnati. 
 
 concinnula Billings, 1865; Pal. Fossils, vol. 1, p. 299. Quebec. 
 
 crepiformis Ulrich, 1879; Jour. Cincinnati Soc. Nat. Hist., vol. 2, p. 10, pi. 7, 
 
 figs. 3, 3 a. 'Hudson. 
 
 [ Cytherina ] cylindrica Hall, 1852; Pal. N. Y., vol. 2, p. 14, pi. 4, figs. 8 a, b. 
 
 For other references, see Isochilina cylindrica. Medina. 
 
 dermatoides Walcott, 1887 ; Am. Jour. Sci., 3d series, vol. 34, p. 192, pi. 1, figs. 
 
 13, 13 a. Cambrian. 
 
 faba Hall, 1876; 28th Rept. New York State Mus. Nat. Hist., Expl., pi. 32, figs. 
 
 1-3. Niagara. 
 
 faba Hall, 1879; 28th Rept. New York State Mus. Nat. Hist., p. 186, pi. 32, 
 
 figs. 1-3 (2d ed.). 
 
 faba Hall, 1882; 11th Aun. Rept. Dept. Geol. Nat. Hist. Indiana, p. 331, pi. 34, 
 
 figs. 1-3, 
 
 [ Cytherina ] fabulites Conrad, 1843; Proc. Acad. Nat. Sci. Phila., vol. 1, p. 332. 
 
 Trenton. 
 
 fabulitea Jones, 1856; Annals Mag. Nat. Hist., London, 2d series, vol. 17, p. 89. 
 
CATALOGUE OF NON-TRILOB ITES. 
 
 V0GDK8.J 
 
 171 
 
 Leperditia fabulites Jones, 1858 ; Annals Mag. Nat. Hist., London, 3d series, vol. 1, 
 p. 341. 
 
 fabulites Jones, 1881 ; Annals Mag. Nat. Hist., London, 4th series, vol. 8, p. 342. 
 
 fabulites Whitfield, 1883; Geol. Wisconsin, vol. 1, p. 60, fig. 5. 
 
 fabulites Jones, 1884 ; Annals Mag. Nat. Hist., London, 5th series, vol. 14, p. 342. 
 
 fonticola, 1867 ; 20th Rept. New York State Cab. Nat. Hist., p. 335, pi. 21, figs. 
 
 1-3. Niagara. 
 
 fonticola, 1870; 20th Rept. New York State Cab. Nat. Hist. (rev. ed.), p. 428, 
 
 pi. 21, figs. 1-3. 
 
 gibbera Jones, 1856; Annals Mag. Nat. Hist., London, 2d series, vol. 17, p. 90, 
 
 pi. 7, figs. 1-3. Niagara. 
 
 gibbera Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 250, 
 
 pi. 10, figs. 7-9. 
 
 gibbera var. scalaris Jones, 1858; Geol. Survey Penn., vol. 2, p. 834, fig. 698. 
 
 gracilis. (See Isochilina gracilis.) 
 
 hudsonica Hall, 1859 ; Pal. New York, vol. 3, p. 375, pi. 79 a, figs. 7 a, b, c. 
 
 Lower Helderberg. 
 
 hudsonica Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 24, pi. 1, figs. 5 a-c, 11 
 
 a-c ; pi. 3, fig. 20 (?) 
 
 jonesi Hall, 1859 ; Pal. New York, vol. 3, p. 272, pi. 79 a, figs. 5 a-e. 
 
 Lower Helderberg. 
 
 jonesi Jones, 1884; Annals Mag. Nat. Hist., London, 5th series, vol. 1, p. 343. 
 
 Syn., alia Hall, 1852 ; Pal. New York, vol. 2, p. 338, pi. 78, figs. 2 a-d. 
 
 josephiana Jones, 1884 ; Annals Mag. Nat. Hist., London, 5th series, vol. 1, p. 341. 
 
 Trenton. 
 
 Syn., canadensis var. josephiana Jones, 1858; Annals Mag. Nat. Hist., London, 3d 
 series, vol. 1, p. 341. 
 
 canadensis var. josephiana Jones, 1858 ; Geol. Survey Canada, decade 3, p. 94, 
 pi. 11, fig. 16. 
 
 fabulites var. josephiana Jones, 1881; Annals Mag. Nat. Hist., London, 5th 
 series, vol. 8, p. 344, pi. 19, fig. 7 ; pi. 20, figs. 7, 8; also, p. 345, pi. 20, fig. 4 (?). 
 labrosa. (See Leperditia canadensis. ) 
 
 louckiana Jones, 1884 ; Annals Mag. Nat. Hist., London, 5th series, vol. 1, p. 341. 
 
 Trenton. 
 
 Syn., canadensis f Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, 
 p. 245, pi. 9, figs. 16, 17. 
 
 Afterwards var. louckiana and Leperditia canadensis var . pauquettiana. 
 canadensis var. louckiana Jones, 1858; Geol. Survey Canada, decade 3, p. 93, 
 pi. 11, fig. 11. 
 
 fabulites var. louckiana Jones, 1881; Annals Mag. Nat. Hist., London, 5th 
 series, vol. 8, p. 343. 
 
 [ Cypridina ] marginata Keyserling, 1846; Wiss. Beob. auf einer Reise in das 
 
 Petochora-Land, p. 288, pi. 11, fig. 16. 
 
 marginata Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 17, p. 
 
 91, pi. 7, figs. 11, 14, 15. 
 
 Syn., Cyridina balthica Eichwald (not Cytherina balthica Hisinger) Bull. Soc. Nat. 
 Moscou, 1854, No. 1, p. 99, pi. 2, fig. 6. 
 
 [ Isochilina] minutissima Hall. (Soe Isochilina minutissima. ) 
 
 morgani Safford; Geol. Tennessee. (Not defined.) 
 
 Nana? Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 27, pi. 4, fig. 4. (See, 
 
 also, Leperditia canadensis var. nana.) 
 
 okeni (Munster) Dawson, 1868; Acadian Geology, p. 256, fig. 78 b. 
 
 Lower Carboniferous. 
 
 Ottawa. (See Isochilina Ottawa.) 
 
 ovata Jones, 1858; Annals Mag. Nat. Hist., London, 3d series, vol. 1, p. 252, pi. 
 
 10, fig. 14. Trenton 
 
172 
 
 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 |bull.63. 
 
 Leperditia ovata Jones, 1858; Geol. Survey Penn., vol. 2, p. 834, fig. 697. 
 
 pauquettiana. (See Leperditia canadensis var. pauquettiana. ) 
 
 parasitica Hall, 1859; Pal. New York, vol. 3, p. 376, pi. 79 a, figs. 8 a, b. 
 
 Lower Helderberg. 
 
 Referred by T. R. Jones to Beyrichia parasitica, which see. 
 
 parvula Hall, 1859 ; Pal. New York, vol. 3, p. 376, pi. 79 a, figs. 9 a, b. 
 
 Lower Helderberg. 
 
 pennsylvanica Jones, 1858; Annajs Mag. Nat. Hist., London, 3d series, vol. 1, p. 
 
 251, pi. 10, figs. 12, 13. Clinton. 
 
 pennsylvanica Jones, 1858 ; Geol. Survey Penn., vol. 2, p. 834, fig. 699. 
 
 punctulifera Hall, 1860; 13th Rept. New York State Cab. Nat. Hist., p. 92. (See 
 
 Primitiopsis punctulifera.) Hamilton. 
 
 radiata Ulrich, 1879; Jour. Cincinnati Soc. Nat. Hist., vol. 2, p. 9, pi. 7, figs. 
 
 2 a, b. Utica. 
 
 rotundata Walcott, 1884; Pal. Eureka Dist., Mon. U. S. Geol. Survey, vol. 8, p. 
 
 206, pi. 16, fig. 5. Devonian. 
 
 scalaris (Leperditia gibbera var. scalaris Jones, 1858) ; Annals Mag. Nat. Hist. 
 
 London, 3d series, vol. 1, p. 250, pi. 10, figs. 7-9. Waterlime. 
 
 seneca Hall, 1861 ; Des. New Species Fossils, p. 84. Hamilton. 
 
 seneca Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 112. 
 
 seneca Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 23, pi. 1, figs. 13, 14. 
 
 sinuata Hall, 1860 ; Canadian Naturalist, vol. 5, p. 158. Upper Silurian. 
 
 sinuata Dawson, 1868; Acadian Geology, p. 609, fig. 217. 
 
 sinuata Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 24, pi. 1, figs. 12 a-c. 
 
 spinulifera Hall, 186\,; Des. New Species Fossils, p. 83. Corniferous. 
 
 spinulifera Hall, 1862; 15th Rept. New York State Cab. Nat. Hist., p. 111. 
 
 [ Cythere ] sublaevis Shumard, 1855; 1st and 2d Ann. Rept. Geol. Survey Mis- 
 souri, p. 195, pi. B, fig. 15. Lower Magnesian. 
 
 subquadrata Jones, 1889; American Geologist, vol. 4, p. 340, pi., figs. 4 a-d. 
 
 Lower Helderberg. 
 
 troyensis Ford. (See Aristozoe troyensis.) 
 
 unicornis Ulrich, 1879 ; Jour. Cincinnati Soc. Nat. Hist., vol. 2, p. 10, pi. 7, figs. 
 
 4, 4 a, b. Hudson. 
 
 Referred by Prof. T. R. Jones to Primitia unicornis. 
 
 ventralis Billings, 1865; Pal. Fossils, vol. 1, p. 300. Quebec. 
 
 Lepidocoleus Faber, 1886; Jour. Cincinnati Soc. Nat. Hist., vol. 9, p. 15. 
 
 jamesi (Hall and Whitfield) Faber, 1886; idem , vol. 9, p. 15, pi. 1, figs. a-f. 
 
 Hudson. 
 
 For other references, see Pumulites jamesi. 
 
 Lisgocaris Clarke, 1882; Am. Jour. Sci., 3d series, vol. 23, p. 478. 
 
 lutheri Clarke, 1882; Am. Jour. Sci., 3d series, vol. 23, p. 478, pi. 1, fig. 5. 
 
 Hamilton. 
 
 Mesothyra Hall, 1888 ; Pal. New York, vol. 7, p. 187. 
 
 [ Dithyrocaris ] neptuni Hall, 1876; Illus. Devonian Fos., pi. 23 (not pi. 22, figs. 
 
 1-5) ; pi. 23, figs. 1-3. Hamilton. 
 
 [ Dithyrocaris ] neptuni Packard, 1878 ; 12th Rept. U. S. Geol. Survey Territories, 
 
 p. 452, fig. 73. 
 
 [ Dithyrocaris ] neptuni Etheridge, Woodward, and Jones, 1887 ; 5th Rept. Comm. 
 
 Foss. Phyllopoda Pal. Rocks, p. 8. 
 
 neptuni Hall, 1888 ; Pal. New York, vol. 7, p. 191, pi. 32, fig. 7 ; pi. 33, fig. 1. 
 
 neptuni Etheridge, Woodward, and Jones, 1888 ; 6th Rept. Comm. Foss. Phyl- 
 lopoda Pal. Rocks, p. 8. 
 
 Syn., oceani Hall, 1888; Pal. New York, vol. 7, p. 187, pi. 32, figs. 1-6; pi. 33, fig. 
 4-7; pi. 34, figs. 1-5. Portage. 
 
 [Dithyrocaris] neptuni Hall, 1876; Illus. Devonian Foss., pi. 22, figs. 1-5; pi. 
 
 33, figs. 1-3. 
 
CATALOGUE OF NON-TRILOBITES. 
 
 VOGDES.] 
 
 173 
 
 Mesothyra IDithyrocaris ] neptuni Etheridge, Woodward, and Jones, 1887 ; 5th Kept. 
 Comm. Foss. Phyllopoda Pal. Rocks, p. 8. 
 
 Syn., Mesothyra oceani Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. 
 Foss. Phyllopoda Pal. Rocks, p. 8. 
 
 atumea Hall, 1888 ; Pal. New York, vol. 7, p. 193, pi. 32, figs. 8, 9 ; pi. 34, fig. 2. 
 
 Hamilton. 
 
 atumea Etheridge, Woodward and Jones, 1888 ; 6th Rept. Comm. Foss. Phyllo- 
 poda Pal. Rocks, p. 8. 
 
 IDithyrocaris ? ] veneris Hall, 1888 ; Pal. New York, vol. 7, p. 193, pi. 33, fig. 3. 
 
 Hamilton. 
 
 IDithyrocaris f J veneris Etheridge, Woodward, and Jones, 1888 ; 6th Rept. Comm. 
 
 Foss. Phyllopoda Pal. Rocks, p. 8. 
 
 Neolimulus Woodward, 1868; Geol. Mag., vol. 5, p. 1. 
 
 Type, Neolimulus falcatus Woodward. 
 
 Nothozoe Barrande, 1872; Syst. Sil. Bohdme, vol. 1, suppl., p. 536. 
 
 Type, Nothozoe pollens Barrande. 
 
 vermontana Whitfield, 1884; Bull. Am. Mus. Nat. Hist., vol. 1, p. 144, pi. 14, 
 
 figs. 14, 15. Potsdam. 
 
 Falaeocaris Meek and Worthen, 1865; Proc. Acad. Nat. Sci. Phila., vol. 17, p. 48. 
 
 typus Meek and Worthen, 1865; Proc. Acad. Nat. Sci. Phila., vol. 17, p. 49. 
 
 Syn., Acanthotelson incequalis Meek and Worthen, 1865; Proc. Acad. Nat. Sci. 
 
 Phila., vol. 17, p. 48. Coal Measures. 
 
 Acanthotelson incequalis Meek and Worthen, 1866 ; Geol. Illinois, vol. 2, p. 403, pi. 
 32, fig. 7, 7 a. 
 
 typus, Meek and Worthen, 1866; Geol. Illinois, vol. 2, p. 405, pi. 32, figs. 5 a-d. 
 
 typus Meek and Worthen, 1868^ Geol. Illinois, vol. 3, p. 552, iigs. a, b. 
 
 typus Peach, 1880 ; Trans. Royal Soc. Edinburgh, vol. 30, p. 85, pi. 10, figs. 
 
 10 g, 10 h. 
 
 typus Brocchi, 1880 ; Bull. Soc. G6ol. France, vol. 8, p. 9, pi. 1, figs. 8-10. 
 
 typus Woodward, 1881 ; Geol. Mag., decade 2, vol. 8, p. 533, wood-cut. 
 
 typus White, 1884 ; 13th Ann. Rept. Dept. Geol. Nat. Hist. Indiana, p. 179, pi. 
 
 38, figs. 1 2, 3. 
 
 typus Packard, 1885; Am. Naturalist, vol. 19, p. 790. 
 
 typus Packard, 1886; Mem. Nat. Acad. Sci., vol. 3, p. 129, pi. 3, figs. 1-4 ; pi. 
 
 7, figs. 1, 2. 
 
 Palceocrangon Salter, 1861. (See Crangopsis Salter, 1863.) 
 
 Palaeopalaemon Whitfield, 1880; Am. Jour. Sci., 3d series, vol. 19, p. 40. 
 
 newberryi Whitfield, 1880; Am. Jour. Sci., 2d series, vol. 19, p. 41. Erie. 
 
 newberryi Whitfielcf, 1880 ; Author’s Edition, plate, figs. 1, 2, 3. 
 
 newberryi Hall, 1888; Pal. New York, vol. 7, p. 203, pi. 30, figs. 20-23. 
 
 Palaeocreusia Clarke, 1888 ; Pal. New York, vol. 7, p. 210. 
 
 devonica Clarke, 1888; Pal. New York, vol. 7, p. 210, pi. 36, figs. 24, 26. 
 
 Corniferous. 
 
 Plumulites Barrande, 1872; Syst. Sil. Boh6me, suppl., vol. 1, p. 565. 
 
 devonicus Clarke, 1882; Am. Journ. Sci., 3d series, vol. 24, p. 55, figs. 1, 2. 
 
 Hamilton. 
 
 jamesi Hall and Whitfield, 1875; Pal. Ohio, vol. 2, p. 106, pi. 4, figs. 1-3. 
 
 Hudson. 
 
 ? jamesi Miller, 1875 ; Cincinnati Quart. Jour. Sci., vol. 2, p. 275, fig. 19. 
 
 Referred by Faber (Jour. Cincinnati Soc. Nat. Hist., vol. 9, 1886, p. 15) to a 
 new genus under the name of Lepidocoleus. 
 
 newberryi Whitfield, 1881 ; Annals New York Acad. Sci., vol. 2, p. 217. 
 
 Huron. 
 
 Prestwichia Woodward, 1867 ; Quart. Jour. Geol. Soc. London, vol. 23, p. 32. 
 
[BULL. 63 . 
 
 174 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Prestwichia danse (Meek and Wortken) Packard, 1886; Mem. Nat. Acad. Sci., vol. 
 3, p. 146, pi. 5, figs. 3, 39 ; pi. 6, figs. 1 a, 2, 2 a. 
 
 For other references to this species, see Euproops and Belinurua. 
 
 eriensis Williams. (See Protolimulus eriensis.) 
 
 Protolimulus Packard, 1866; Mem. Nat. Acad. Sci., vol. 3, p. 150. 
 
 [Prestwichia ] eriensis Williams, 1885 ; Am. Jour. Sci., 3d series, vol. 30, p. 45, 
 
 3 figs. Devonian. 
 
 [Protolimulus') eriensis Packard, 1886; Mem. Nat. Acad. Sci., vol. 3, p. 150, 
 
 figs. 11-13. 
 
 eriensis Hall, 1888 ; Pal. New York, vol. 7, p. 153, pi. 26, figs. 1, 2. 
 
 Primitia Jones and Holl, 1865; Annals Mag. Nat. Hist., 3d series, London, vol. 16, p. 
 415. 
 
 Primitia cristata Whitfield, 1889; Bull. Am. Mus. Nat. Hist., New York, vol. 2, p. 59, 
 pi. 13, figs. 1, 2. (See Isochilina cristata.) 
 
 gregaria Whitfield, 1889; Bull. Am. Mus. Nat. Hist., New York, vol. 2, p. 58, pi. 
 
 13, figs. 3-5. (See Isochilina gregaria.) 
 
 lativia Ulrich, '1889 ; Contributions Micro-Palaeont., pt. 2, p. 50, pi. 9, figs. 8, 8 a. 
 
 Hudson. 
 
 [Beyrichia) loganix ar. leperditioides Jones, 1858; Annals and Mag. Nat. Hist., 
 
 London, 3d series, vol. 1, p. 244, pi. 9, fig. 10. Trenton. 
 
 [Beyrichia) logani var. leperditoides Jones, 1858; Geol. Survey Canada, decade 
 
 3, p. 91, pi. 11, figs. 1-5. 
 
 leperditioides Jones, 1884 : Annals and Mag. Nat. Hist., 6th series, London, 
 
 vol. 14, p. 345. 
 
 mundula Jones, 1889; American Geologist, vol. 4, p. 337, pi., figs. 1,2, 10, 15. 
 
 Upper Devonian. 
 
 [Beyrichia (Primitia)) occidentalis Walcott, 1884 ; Pal. Eureka Diet., Mon. U. S. 
 
 Geol. Survey, vol. 8, p. 204, pi. 17, figs. 4, 4 a. Devonian. 
 
 [Beyrichia?) parallels Ulrich, 1889; Contributions Micro-PalaBont., pt. 2, p. 51, 
 
 pi. 9, figs. 7-7 a. Hudson. 
 
 pennsylvanica Jones, 1889 ; American Geologist, vol. 4, p. 339, pi., figs. 15 a, b. 
 
 Marcellus. 
 
 seminulum Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 5, pi. 2, fig. 2. 
 
 Hamilton. 
 
 seelyi Whitfield, 1889; Bull. Am. Mus. Nat. Hist., N. Y., vol. 2, p. 60, pi. 13, figs. 
 
 15-21. (See Isochilina seelyi.) 
 
 unicornis (Ulrich) Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 7, pi. 11, figs. 
 
 8-13. 
 
 For other references, see Beyrichia unicornis Ulrich. The species is referred 
 by Ulrich (Contributions Micro-Palseont., pt. 2, p. 50) to Aparchites unicornis, 
 pi. 9, fig. 11. 
 
 whitfieldi Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 9, pi. 3, figs. 24 a, b. 
 
 Cincinnati. 
 
 Primitiopsis Jones, 1887 ; Notes on some Sil. Ostracoda from Gothland, p. 5. 
 
 punctulifera (Hall) Jones, 1890 ; Quart. Jour. Geol. Soc., vol. 46, p. 9, pi. 2, figs. 
 
 7 a, b, 12 a, b. * Hamilton. 
 
 For other references, see Beyrichia punctulifera Hall. 
 
 Protobalanus Whitfield, 1889; Bull. Am. Mus. Nat. Hist., New York, vol. 2, p. 66; 
 Hall, 1888; Pal. New York, vol. 7, pp. lxii and 209. 
 
 hamiltonensis (Whitfield) Hall, 1888 ; Pal. New York, vol. 7, p. 209, pi. 36, fig. 23. 
 
 hamiltonensis Whitfield, 1889 ; Bull. Am. Mus. Nat. Hist., New York, vol. 2, p. 67, 
 
 pi. 13, fig. 22. Marcellus. 
 
 Protocaris Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 50. 
 
 marshi Walcott, 1884; Bull. U. S. Geol. Survey, No. 10, p. 50, pi. 10. 
 
 Cambrian, 
 
 • marshi Walcott, 1886 ; Bull. U. S. Geol. Survey, No. 30, p. 148, p\, 15, fig. 1, 
 
V0GDE8.] 
 
 CATALOGUE OF NON-TRI LOBITES. 
 
 175 
 
 Pterygotus Agassiz, 1844 ; Mon. Poissons Fossiles, note, p. xix. 
 
 acuticauda Pohlman, 1882 ; Ball. Buffalo Soc. Nat. Sci., vol. 4, p. 42, pi. 2, 
 
 fig. 3. Waterlime. 
 
 bilobus (Huxley and Salter) Pohlman, 1886 ; Bull. Buffalo Soc. Nat. Sci., vol. 
 
 5, p. 27. Waterlime. 
 
 buffaloensis Pohlman, 1881 ; Bull. Buffalo Soc. Nat. Sci., vol. 4, p. 17, figs. 1,2. 
 
 Waterlime. 
 
 buffaloensis Pohlman, 1882 ; Bull. Buffalo Soc. Nat. Sci., vol. 4, p. 44, pi. 3, 
 
 fig. 3. 
 
 buffaloensis Pohlman, 1886; Bull. Buffalo Soc. Nat. Sci., vol. 5, p. 24, pi. 3, fig. 1. 
 
 canadensis Dawson, 1881; Canadian Naturalist, new series, vol. 9, p. 103, figs. 
 
 1,2. Niagara. 
 
 cobbi Hall, 1859; Pal., New York, vol. 3, p. 417, pi. 83 b, fig. 4; pi. 84, fig. 8 (?). 
 
 Waterlime. 
 
 cummingsi Grote and Pitt, 1875; Bull. Buffalo Soc. Nat. Sci., vol. 3, p. 18, figure. 
 
 Waterlime. 
 
 cummingsi Grote and Pitt, 1878 ; Proc. Am. Assoc. Adv. Sci., 26th Meeting, p. 
 
 300, figure. 
 
 globicaudatus Pohlman, 1882 ; Bull. Buffalo Soc. Nat. Sci., vol. 4, p. 42, pi. 2, 
 
 fig. 2. Waterlime. 
 
 macrophthalmus Hall, 1859; Pal. New York, vol. 3, p. 418, pi. 80 a, figs. 8,8 a. 
 
 Waterlime. 
 
 macrophthalmus Pohlman, 1882; Bull. Buffalo Soc. Nat. Sci., vol. 4, p. 44. 
 
 osborni Hall, 1859; Pal. New York, vol. 3, p. 419, pi. 80 a, fig. 9. Waterlime. 
 
 quadricaudatus Pohlman, 1882; Bull. Buffalo Soc. Nat. Sci., vol. 4, p. 43, pi. 3, 
 
 fig. 1. Waterlime. 
 
 Eachura Scndder, 1878; Proc. Boston Soc. Nat. Hist., vol. 19, p. 296. 
 
 Probably the same as the genus Dithyocaris. 
 
 venom Scudder, 1878; Proc. Boston Soc. Nat. Hist., vol. 19, p. 296. 
 
 Coal Measures. 
 
 [ Dithyocaris t ] venosa Etheridge, Woodward, and Jones, 1888; 6th Kept. Comm. 
 
 Foss. Phyllopoda, p. 4. 
 
 Rhinocaris Clarke, 1888; Pal. New York, vol. 7, p. lviii. 
 
 columbina Clarke, 1888 ; Pal. New York, vol. 7, p. 195, pi. 31, figs. 16-21. 
 
 Hamilton. 
 
 columbina Etheridge, Woodward, and Jones, 1888 ; 6th Rept. Comm. Foss. Phyl- 
 lopoda, etc., p. 8. 
 
 acaphoptera Hall, 1888; Pal. New York, vol. 7, p. 197, pi. 31, figs. 22, 23. 
 
 Hamilton. 
 
 acaphoptera Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 8. 
 
 Schizodiscua Clarke, 1888 ; Pal. New York, vol. 7, p. 207. 
 
 capra Clarke, 1888; Pal. New York, vol. 7, p. 207, pi. 25, figs. 1-9. Hamilton. 
 
 SpathiocariB Clarke, 1882; Am. Jour. Sci., 3d series, vol 23, p. 477. 
 
 emersoni Clarke, 1882; Am. Jour. Sci., 3d series, wol. 23, p. 477, pi., figs. 1-3. 
 
 Hamilton. 
 
 emersoni Packard, 1883; 12th Rept. U. S. Geol. Survey Territories, p. 451. 
 
 emersoni Clarke, 1886; Neues Jarbuch fiir Mineral., p. 180. 
 
 emersoni Woodward and Jones, 1884; 2d Rept. Comm. Foss. Phyllopoda Pal. 
 
 Rocks, p. 7. 
 
 emersoni Clarke, 1885; Bull. U. S. Geol. Survey, No. 16, p. 46. 
 
 emersoni Etheridge, Woodward, and Jones, 1885 ; 3d Rept. Comm. Foss. Phyllo- 
 poda Pal. Rocks, p. 3. 
 
 emersoni Ilall, 1888; Pal. New York, vol. 7, p. 199, pi. 35, figs. 12-18. 
 
 emersoni Etheridge, Woodward, and Jones, 1888; 6th Rept. Comm. Foss. Phyl- 
 lopoda Pal. Rocks, p. 8, 
 
[BULL. 63 . 
 
 176 A BIBLIOGRAPHY OF PALEOZOIC CRUSTACEA. 
 
 Solenocaris Meek, 1871; Proc. Acad. Nat. Sci. Phila., vol. 23, p. 335. 
 
 The name Solenocaris was used for a species of fossil Crustacea by Mr. J. Young 
 in 1868. Change to Strigocaris. 
 
 ludovici Worthen, 1884; Bull. Illinois State Cab. Nat. Hist., No. 2, p. 3. 
 
 St. Louis. 
 
 [Ceratiocaris ( Solenocaris )] strigata Meek, 1872; Proc. Acad. Nat. Sci. Phila., vol. 
 
 23, p. 335. Waverly. 
 
 [Ceratiocaris ( Solenocaris )] strigata Meek, 1875; Pal. Ohio, vol. 2, p. 321, pi. 18, 
 
 figs. 4 a-c. 
 
 Strigocaris, name suggested to replace preoccupied generic name Solenocaris (Meek) 
 Vogdes, 1889; Annals N. Y. Acad. Sci., vol. 5, p. 34. 
 
 [Solenocaris] st. ludovici Worthen, 1884; Bull. Illinois State Cab. Nat. Hist., 
 
 No. 2, p. 3. St. Louis. 
 
 [Ceratiocaris (Solenocaris)] strigata Meek, 1872; Proc. Nat. Acad. Sci. Phila., 
 
 vol. 23, p. 335. Waverly. 
 
 [Ceratiocaris ( Solenocaris )] strigata Meek, 1875; Pal. Ohio, vol. 2, p. 321, pi. 18, 
 
 figs. 4 a-c. 
 
 Strobilepsis Clarke, 1888 ; Pal. New York, vol. 7, p. 212. 
 
 spinigera Clarke, 1888 ; Pal. New York, vol. 7, p. 212, pi. 36, figs. 20-22. 
 
 Hamilton. 
 
 Stylonurus Page, 1856; Advance Text-book Geology. 
 
 excelsior Hall, MSS. Catskill. 
 
 excelsior Martin, 1882; Trans. New York Acad. Sci., vol. 2, p. 8. 
 
 excelsior Hall, 1884 ; 36th Rept. New York State Mus., p. 77, pi. 5, fig. 1. 
 
 excelsior Hall, 1885 ; Proc. Am. Assoc. Adv. Sci., 33d Meeting, p. 421. 
 
 excelsior Hall, 18£$3 ; Pal. New York, vol. 7, p. 156, pi. 26 ; also p. 221, pi. 26 a. 
 
 Compare Dolichocephala lacoana Claypole. 
 
 [Equistides] wrightianus Dawson, 1881 ; Quart. Jour. Geol. Soc., vol. 37, p. 303, 
 
 pi. 12, fig. 10; pi. 13, fig. 20. Portage. 
 
 [Equistides] wrightianus (Dawson) Wright ; 35th Rept. New York State Mus. 
 
 Nat. Hist., Expl., pi. 15, note, figs. 1,2. 
 
 [Echinocaris] wrightianus Jones and Woodward, 1684; Geol. Mag., decade 3, 
 
 vol. 1, p. 3, pi. 13, figs. 1 a, b. 
 
 [Echinocaris] wrightianus Etheridge, Woodward, and Jones, 1885 ; 3d Rept. 
 
 Comm. Fossil Phyllopoda Pal. Rocks, p. 35. 
 
 ? [Echinocaris] wrightianus Hall, 1888; Pal. New York, vol. 7, p. 160, pi. 27, 
 
 figs. 7-9. 
 
 Strepula Jones and Holl, 1886; Annals Mag. Nat. Hist., 5th series, London, vol. 17, 
 p. 403. 
 
 lunatifera Ulrich, 1889; Contributions Micro-Palseont., pt. 2, p. 56, pi. 9, tigs. 
 
 14, 14 b. Hudson. 
 
 quadrilirata (Hall and Whitfield) Ulrich, 1889; Contributions Micro-Palseont., 
 
 pt. 2, p. 54, pi. 9, fig. 12. 
 
 For other references, see Beyrichia quadrilirata. 
 
 sigmoidalis Jones, 1890; Quart. Jour. Geol. Soc., vol. 46, p. 11, pi. 2, fig. 4. 
 
 Hamilton. 
 
 Tropidocaris Beecher, 1884 ; 2d Geol. Survey Pennsylvania, vol. PPP, p. 15. 
 
 alternata Beecher, 1884 ; 2d Geol. Survey Penn., vol. PPP, p. 19, pi. 2, figs. 7, 8. 
 
 Chemung. 
 
 alternata Etheridge, Woodward, and Jones, 1885; 3d Rept. Comm. Fobs. Phyllo- 
 
 poda Pal. Rocks, p. 35. 
 
 alternata Hall, 1888; Pal. New York, vol. 7, p. 186, pi. 31, figs. 14, 15. 
 
 bicarinata Beecher, 1884; 2d Geol. Survey Penn., vol. PPP, p. 16, pi. 2, figs. 3-5. 
 
 Chemung. 
 
 bicarinata Etheridge, Woodward, and Jones, 1885; 3d Rept. Comm. Foss. Phyl- 
 lopoda Pal. Rocks, p. 35. 
 
V0GDE6.] 
 
 CATALOGUE OF NON-TRILOBITES. 
 
 177 
 
 Tropidocaris bicarinata Hall, 1888 ; Pal. New York, vol. 7, p. 184, pi. 31, figs. 7-12. 
 
 Interrupta Beecher, 1884; 2d Geol. Survey Penn., vol. PPP, p. 18, pi. 2, fig. 5. 
 
 Chemung. 
 
 interrupta Etheridge, Woodward, and Jones, 1885 ; 3d Kept. Comm. Foss. 
 
 Phyllopoda Pal. Rocks, p. 35. 
 
 interrupta Hall, 1888 ; Pal. New York, vol. 7, p. 185, pi. 31, figs. 7-12. 
 
 Turrilepas Woodward, 1865 ; Quart. Jour. Geol. Soc., vol. 21, p. 489. 
 
 cancellatus Hall, 1888 ; Pal. New York, vol. 7, p. 216, pi. 36, fig. 2. 
 
 Corniferous. 
 
 [ Plumulites] devonicus Clarke, 1882; Am. Jour. Sci., 3d series, vol. 24, p. 55, 
 
 figs. 1,2. Hamilton. 
 
 devonicus Hall, 1888 ; Pal. New York, vol. 7, p. 215, pi. 36, fig. 1. 
 
 flexuosus Hall, 1888; Pal. New York, vol. 7, p. 215, pi. 36, fig. 1. Corniferous. 
 
 foliatus Hall, 1888; Pal. New York, vol. 7, p. 218, pi. 36, fig. 15. Hamilton. 
 
 [ Plumulites ] newberryi Whitfield, 1882 ; Annals New York Acad. Sci., vol. 2, 
 
 p. 217. Hamilton. 
 
 newberryi Hall, 1888; Pal. New York, vol. 7, p. 219, pi. 36, figs. 16-19. 
 
 nitidulus Hall, 1888; Pal. New York, vol. 7, p. 218, pi. 36, fig. 4. Hamilton. 
 
 squama Hall, 1888 ; Pal. New York, vol. 7, p. 217, pi. 36, figs. 5-8. Hamilton. 
 
 tener Hall, 1888 ; Pal. New York, vol. 7, p. 219, pi. 36, figs. 9-14. Hamilton. 
 
 Bull. 63 12 
 
 © 
 
Title for subject entry. Author title. Series title, 
 
 LIBRARY CATALOGUE SLIPS. 
 
 United States. Department of the interior. ( U. S. geological survey ). 
 
 Department of the interior [ — | Bulletin | of the | United 
 States ! geological survey | no. 64 | [Seal of the department] | 
 
 Washington | government printing office | 1890 
 
 Second title: United States geological survey | J. W. Powell, 
 director | — | A report of work done | in the | division of chem- 
 istry and physics | mainly during the | fiscal year 1888-’89 | — f 
 F. W. Clarke, chief chemist | [Vignette] j 
 
 Washington | government printing office | 1890 
 
 8°. 60 pp. 
 
 Clarke (Frank Wiggles worth). 
 
 United States geological survey | J. W. Powell, director | — | 
 A report of work done | in the | division of chemistry and physics | 
 mainly during the | fiscal year 1888-89 | — | F. W. Clarke, chief 
 chemist | [Vignette] | 
 
 Washington | government printing office | 1890 
 
 8°. 60 pp. 
 
 [United States. Department of the interior. (U. S. geological survey). 
 
 Bulletin 64]. 
 
 United States geological survey | J. W. Powell, director | — | 
 A report of work done | in the | division of chemistry and physics | 
 mainly during the | fiscal year 1888-89 | — | F. W. Clarke, chief 
 chemist | [Vignette] | 
 
 Washington | government printing office | 1890 
 
 8°. 60 pp. 
 
 [United States Department of the interior. (77. S. geological survey). 
 
 Bulletin 64.] 
 
ADVERTISEMENT 
 
 [Bulletin No. 64.] 
 
 The publications of the United States Geological Survey are issued in accordance with the statute 
 approved March 3, 1879, which declares that— 
 
 “ The publications of the Geological Survey shall consist of the annual report of operations, geological 
 and economic maps illustrating the resources and classification of the lands, and reports upon general 
 and economic geology and paleontology. The annual report of operations of the Geological Survey 
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 Washington, D. C., June , 1890. 
 
DEPARTMENT OF THE INTERIOR 
 
 BULLETIN 
 
 OF THE 
 
 UNITED STATES 
 
 GEOLOGICAL SURVEY 
 
 3STo. 64 
 
 WASHINGTON 
 GOVERNMENT PRINTING OFFICE 
 1890 
 
UNITED STATES GEOLOGICAL SURVEY 
 
 J. W. POWELL, DIRECTOR 
 
 A REPORT OF WORK DONE 
 
 # 
 
 IN THE 
 
 DIVISION OF CHEMISTRY AND PHYSICS 
 
 MAINLY DURING THE 
 
 FIS CAL YEAR 1888-’89 
 
 WASHINGTON 
 
 GOVERNMENT PRINTING OFFICE 
 1890 
 
CONTENTS 
 
 Page. 
 
 Preface 7 
 
 A theory of the mica group. By F. W. Clarke 9 
 
 A platiniferous nickel ore from Canada. By F. W. Clarke and Charles Catlett. 20 
 
 A new occurrence of gyrolite. By F. W. Clarke 22 
 
 Analyses of three descloizites from new localities. By W. F. Hillebrand 24 
 
 A new meteorite from Mexico. By J. E. Whitfield 29 
 
 Dumortierite from Harlem, N. Y., and Clip, Ariz. By J. S. Diller and J. E. 
 
 Whitfield 31 
 
 Chemical action between solids. By William Hallock 34 
 
 The flow of solids; a note. By William Hallock 38 
 
 Miscellaneous analyses 40 
 
 5 
 
 i 
 
 
PREFACE. 
 
 The present bulletin represents work finished in the Division of 
 Chemistry and Physics during the fiscal year 1888-’89, and resembles 
 in general design and purpose its predecessors, Nos. 9, 27, 42, 55, and 
 60. It covers, however, only a part of the work actually accomplished, 
 for some investigations are not yet completed, others will appear in 
 special bulletins now in course of preparation, and many analyses will 
 be published in forthcoming reports of the field geologists. 
 
 F. W. Clarke, 
 
 Chief Chemist 
 
WORK DONE IN THE DIVISION OF CHEMISTRY AND 
 PHYSICS IN 1888-89. 
 
 A THEORY OF THE MICA GROUP. 
 
 By F. W. Clarke. 
 
 Ever since its publication in 1878, 1 in spite of a few dissentient 
 voices, Tschermak’s theory of the mica group has been generally in 
 vogue. Nevertheless, upon careful inspection, the theory seems open 
 to serious objections. In brief, omitting details for the present, 
 Tschermak regards the micas as made up of four fundamental mole- • 
 cules; to which the following formulae are assigned: 
 
 1. R' 6 Al 6 Si 6 0 24 . 
 
 2. Mg 14 Si 6 0 24 . 
 
 3. HgSiioO^. 
 
 4. F 2 4Siio0 8 . 
 
 B' stands obviously for K, Na, Li, or H ; Mg is equivalent to Fe", and 
 aluminum may be replaced by ferric iron. The first of these formulae 
 represents fairly well the composition of normal muscovite and para- 
 gonite ; the only objection to it being that, as used by Tschermak, it as- 
 sumes the double atom of quadrivalent aluminum. Since it has been 
 proved by Nilson and Petterson, Combes, Quincke, and others, that 
 aluminum is truly trivalent, the formula should become B^A^S^O^; 
 which, as I have shown in several previous papers, may be regarded as 
 a substitution derivative of normal aluminum orthosilicate. 
 
 The second, third, and fourth of Tschermak’s formulae represent 
 hypothetical compounds, the second being a polymer of chrysolite, to 
 which, in nature, some varieties of talc offer the nearest approximation. 
 The third and fourth formulae are analogous to no known substances, 
 and are, moreover, improbable chemically. No mica, by itself, resembles 
 in composition either of the three. One formula, then, corresponds to 
 an observed mineral, while the others are purely speculative ; a state 
 of affairs which is not altogether satisfactory. Furthermore, the four 
 formulae represent as many distinct chemical types, whereas it would 
 seem as if all the true micas should be reducible to one general form, 
 under which their isomorphism would be more readily intelligible. 
 
 l Ber. Wien. Akad., vol. 78, p. 5. Zeitschr. Kryst., vol. 3, p. 122. 
 
 9 
 
10 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 64 . 
 
 There is still another objection to Tschermak’s system of formulae, 
 which, if sustained by future investigation, will be fatal. XJnder his 
 theory the ratio of oxygen to silicon in the micas can never exceed four 
 to one; while the published analyses of micas often show values far 
 higher, ranging in some cases nearly up to five. In certain instances, 
 as Tschermak himself suggests, this excess of oxygen over the ortho* 
 silicate ratio may be due to water inclosed between micaceous laminae; 
 and in other cases it may indicate partial alteration. There are micas, 
 however, in which neither of these explanations appears to be satisfac- 
 tory, and the weight of evidence goes to show that the excess of 
 oxygen is essential. If this be true, Tschermak’s theory is so far inade- 
 quate, for to such micas it can not apply without serious modification. 
 The question can only be settled experimentally, but at present the 
 objection raised by it can not be ignored. Some of its details will be 
 considered later. 
 
 jSTow, in order to conclusively replace Tschermak’s theory by some- 
 thing better, two fundamental conditions must be satisfied. First, all 
 micas, with the possible exception of the pseudomica, margarite, should 
 be reducible to one general type of formula, which shall express all 
 known relations equally well with the formulae proposed by Tschermak. 
 Secondly, hypothetical compounds must be so far as possible avoided, 
 and admitted into consideration only when their assumption can be 
 shown to be absolutely necessary. The chief difficulties to be over- 
 come are the variations in the silicon -oxygen ratio, and the presence of 
 fluorine in many common micas. 
 
 In a number of papers published during the past four years, 1 1 have 
 sought to show that all orthosilicates containing aluminum may be 
 represented as substitution derivatives of the normal salt Al 4 (Si0 4 ) 3 . 
 Muscovite can be so derived, theoretically, through the replacement of 
 one aluminum atom by R' 3 ; and in many other cases we have equal 
 simplicity of expression. The ferro- magnesian micas, the phlogopites, 
 and the lepidolites, however, are less simply derived; and I have in 
 certain cases suggested a linking together of two orthosilicate nuclei 
 to the group Al 2 (Si0 4 ) 5 in order to account for their formation. I am 
 now inclined to believe, however, that all the true micas are referable 
 to the same general type, and have discussed nearly one hundred 
 published analyses from that point of view. If we take magnesium as 
 a generic representative of the bivalent metals, and give univalent 
 elements or groups the general symbol R, we can imagine the following 
 derivatives of Al 4 (Si0 4 ) 3 as easily possible: 
 
 l. 
 
 Si0 4 E R: 
 Al — Si0 4 
 \i0 4 ~A1 
 
 Al 
 
 2 . 
 
 Si0 4 E Rs 
 
 Al — Si0 4 =R 3 
 
 \ 
 
 Si0 4 E Al 
 
 3. 
 
 Si0 4 — R 3 
 
 / 
 
 Al — Si0 4 = R3 
 
 \ 
 
 Si0 4 — R 3 
 
 ' Am. Jour. Sci., Nov., 1886, and Aug., 1887. Also, Am. Cbem. Jour., vol. 10, p. 120 
 (March, 1888). 
 
CLARKE.] 
 
 A THEORY OF THE MICA GROUP. 
 
 11 
 
 Al — Si0 4 EAl 
 
 Si0 4 = MgR 
 
 4. 
 
 5. 
 
 Si0 4 EE MgR 
 Al — Si0 4 =MgR 
 Si0 4 EE Al 
 
 To these we may add, as No. 7, the compound Al 2 (Si0 4 )6Mg 9 , the biv- 
 alent analogue of No. 3, and identical in type with it. Now, so long as 
 we have only orthosilicate micas to consider, these seven formulae cover 
 all their variations in composition ; provided that fluorine, when pres- 
 ent, is represented either by — Mg— F or -A1=F 2 , univalent groups 
 which are included under the general symbol IF. Most of the micas 
 appear as intermediate mixtures of these presumably isomorphous types. 
 No. 1 represents muscovite and paragonite, and No. 6 agrees tolerably 
 with some phlogopites. No. 2 may be resolved into a mixture, in equal 
 molecules, of No. 1 and 3 ; and similarly No. 5 may be regarded as com- 
 posed of Nos. 4 and 6. Nos. 5 and 6, moreover, may be simplified into 
 mixtures between 3 and 7, so that numbers 1, 3, 4, and 7 represent all 
 the necessary relations. Even No. 4 is possibly superfluous. 
 
 So much for the normal orthosilicate micas. But in the lepidolites, 
 phlogopites, and some muscovites, the oxygen silicon ratio is low ; and 
 in the lepidolites especially it approximates more or less closely to the 
 metasilicate type. This order of variation is clearly established, while 
 variations in the opposite direction, that is toward excess of oxygen, 
 may be questionable. If, however, in any mica the oxygen can be 
 properly in excess of Si0 4 , that excess may be fairly regarded as present 
 in the group — A1=0, which is obviously equivalent to Al=F 2 , and 
 takes place with the latter as a part of IF. Examples of this kind are 
 given in one of my former papers. 1 In all such cases the system of 
 formulae proposed above applies perfectly, and needs no qualification. 
 The variations in B/ always fall within its limits. 
 
 The lower values for the silicon -oxygen ratios are explicable as follows: 
 The polysilicic acid H 4 Si 3 0 8 , which, like H 4 Si0 4 is tetrabasic, is repre- 
 sented in nature by orthoclase and albite. In anorthite we have an 
 orthosilicate, and its mixture with albite gives, as is well known to all 
 mineralogists, the intermediate tricliuic feldspars in which pseudo-meta- 
 silicate ratios often appear. H 4 Si 3 0 8 +H 4 Si0 4 =H 8 Si 4 0i 2 == 4H 2 Si0 3 . It 
 we assume a similar state of affairs among the micas, and regard ortho- 
 silicates and poly silicates as isomorphously miscible, the lepidolites 
 and other low oxygen micas are completely accounted for. We have 
 then the same system of general formulae for all micas, the normal salts 
 Al 4 (Si0 4 ) 3 and Al 4 (Si 3 0 8 ) 3 being the theoretical starting points for deri- 
 vation. In every case the composition of a mica becomes reducible to 
 the one general type, under the proposed theory of substitution. Repre- 
 senting the groups Si0 4 and Si 3 0 8 by the common symbol X, the micas 
 all fall within limits indicated by the formulae A1 3 X 3 1F 3 , and A1X 3 IF 9 . 
 We may test this principle and the preceding formulae by application 
 to actual examples, taking the different micas group by group. 
 
 1 Am. Jour. Sci., Aug,, 1887, p. 131. 
 
12 
 
 WASHINGTON LABORATORY. 
 
 | BULL. 64. 
 
 MUSCOVITE. 
 
 This mica, the most typical and most abundant of all, is also the 
 simplest chemically. It is best represented by formula No. 1, which, 
 in its special application, becomes ordinarily Al 3 (Si 0 4 ) 3 KH 2 , with some 
 variation in the ratio of K to H. In most cases muscovite contains 
 small amounts of magnesia and ferrous iron $ and if these are deducted, 
 as shown in formula No. 6, the residue agrees still better with formula 
 No. 1. Fluorine is often present in small quantities, and appears to 
 vary in relation to hydrogen, being the lowest when the latter is high, 
 and the reverse. Hence it is probable that the group A1F 2 replaces H 
 rather than K. This is shown more clearly among the lepidolites, in 
 which fluorine reaches a maximum, while the proportion of water is 
 almost insignificant. 
 
 Some muscovites, however, vary from the normal compound in that 
 they contain more silicon and less oxygen ; thus approaching somewhat 
 to lepidolite. These micas, which Tschermak has called u phengites,” 
 are represented by him as mixtures of Al 6 R / 6 Si 6 0 2 4 with H 8 Sii 0 O 24 in the 
 ratio of three to one. It is simpler, however, to follow out the analogy 
 offered by the feldspar group, and to assume the existence in muscovite 
 of the isomorphous compound Al3(Si 3 0 8 ) 3 KH2. True, this compound 
 has not been found by itself in nature, and so far its assumption is 
 objectionable. But the compound H 8 Si ]0 O 24 is also non-existent, is 
 different in type from ordinary muscovite, and is not easily conceivable 
 as a definite entity. The alternative which I offer for it is therefore, it 
 seems to me, more philosophical and more satisfactory ; and it accounts 
 completely for all the oxygen variations in muscovite. For the sake of 
 brevity, however, we may well retain the name of phengite in our 
 vocabulary, and may speak of micas containing the Si 3 0 8 group as 
 more or less phengitic. 
 
 In order to show the method of discussion which I have employed, 
 we may take the four muscovite analyses considered by Tschermak. A, 
 muscovite from Bengal, analyzed by Blau ; B, East Indies, by Sipocz ; 
 C, Bothenkopf in the Zillerthal, by Sipocz ; D, Soboth in Steiermark, 
 by Lobisch. Of these, C and D are phengites. 
 
 
 A. 
 
 B. 
 
 C. 
 
 I). 
 
 Si0 2 
 
 45.57 
 
 45. 71 
 
 45. 87 
 
 48.76 
 
 AI 2 O 3 
 
 36. 72 
 
 36.57 
 
 30. 86 
 
 29. 91 
 
 Fe 2 0 a 
 
 .95 
 
 1.19 
 
 5. 70 
 
 4. 24 
 
 FeO 
 
 1.28 
 
 1.07 
 
 1. 69 
 
 .41 
 
 MgO 
 
 .38 
 
 .71 
 
 1.56 
 
 2.63 
 
 CaO 
 
 .21 
 
 .46 
 
 .23 
 
 .33 
 
 K 2 0 
 
 8. 81 
 
 9.22 
 
 9.07 
 
 6.83 
 
 Xa 2 0 
 
 .62 
 
 .79 
 
 .54 
 
 2. 31 
 
 Li 2 0 
 
 . 19 
 
 
 
 
 H 2 0 
 
 5.05 
 
 4.83 
 
 4.60 
 
 4. 60 
 
 F 
 
 .15 
 
 . 12 
 
 
 
 
 
 
 
 
 
 99. 93 
 
 100. 67 
 
 100. 12 
 
 100 . 02 
 
CLARKE. J 
 
 A THEORY OF THE MICA GROUP. 
 
 13 
 
 •Now, computing the molecular ratios in the usual way, uniting ferric 
 oxide with alumina, ferrous iron and lime with the magnesia, and con- 
 solidating the alkalies under the general symbol R' 2 0, we have the 
 following empirical formulae for the four micas : 
 
 A. Al732Mg3oR / 22oH56oF eSbsgCbiE?* 
 
 B . Al732Mg39R / -2.22H53fiF gSi 7620.3037° 
 
 C . A1 676 M g6sR '21 2 H 5 12 S i 765 O 2972 • 
 
 D. Al634Mg7 8 R / 220H5l2Si813O302l° 
 
 Regarding the fluorine as A1F 2 , and uniting it and the H with R', 
 these formulae become, almost exactly : 
 
 A. Al729Mg3oR / 783(Si04)753(Si308)2° 
 
 B. AbagMgsgRbei (Si 
 
 C . Alfi76Mge6R / 724( Si04)699( S^Og^. 
 
 D. Al634Mg7sR'732(Si04)642(Si308)67* 
 
 Combining the two acid groups under the indiscriminate symbol X, 
 we have : 
 
 A. Al729Mg3oR / 783X755. 
 
 B. Al729Mg39R'76lX766. 
 
 C. Al«76Mg66R / 724X72l. 
 
 D. . Al634Mg78R / 732X699« 
 
 These are equivalent to the following mixtures of the isomorphous 
 salts represented by the general formulae 6, 3, and 1, in the fundamental 
 system above cited : 
 
 A. 10 AlX 3 Mg3R / 3 +4 AlX 3 R' 9 +238 AhXsR's. 
 
 B. 13 AlX3Mg 3 R / 3 +239 AI 3 X 3 R?. 
 
 C. 22 AlX 3 Mg 3 R'3+218 A1 3 X 3 R'3. 
 
 D. 26 AIXaMggR's-f 7 AlX 3 R / 9+200 A1 3 X 3 R'3. 
 
 In each case the final formulae vary from the original ratios only to 
 an extent which is ascribable to the minute residual errors of calcula- 
 tion. The new expressions conform perfectly to the evidence of analysis. 
 Eight other muscovite analyses, similarly discussed, gave strictly 
 similar and equally sharp results. 
 
 LEPIDOLITE. 
 
 In this species, the most phengitic of all the micas, we find little 
 water, high fluorine, and a very notable proportion of lithia. It always 
 occurs with muscovite, and commonly implanted upon the latter in 
 such a way as to clearly indicate its later formation. In composition it 
 is regarded by Tschermak as a mixture of Al fi K 6 Si 6 0 2 4 with F 24 Sii 0 O 8 , 
 the former being about half replaced by the corresponding Al 6 Li 6 Si 6 0 24 , 
 and the latter in part by H 8 Sii 0 O 2l . The objections to this interpreta- 
 tion have already been pointed out. 
 
 Under the new mode of interpretation, lepidolite becomes much 
 simpler. In every case, if we eliminate traces of magnesia and iron, 
 as was done under muscovite, the residue corresponds sharply to a 
 mixture of the two molecules AlX 3 R / 9 with Al ; ,X :i R'j, X representing 
 
14 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 64. 
 
 Si 3 0 8 and Si0 4 indiscriminately. In the purest lepidolites these mole- 
 cules are in the ratio 1 : .1, corresponding to A1 2 X 3 R' 6 ; but in general 
 the second molecule is slightly in excess, due to small admixtures of 
 normal muscovite. In the discussion of fourteen published analyses 
 of lepidolite the ratio Si 3 0 8 :Si0 4 varies from 1 : 1 to 1 : 3; and the sum 
 of Li+A1F 2 appears to be directly related to the proportion of Si 3 O e . 
 In brief, expanding the general formulae given above, typical lepidolite 
 may be expressed by the two compounds Al 3 (Si0 4 ) 3 KHLi and 
 Al(Si 3 0 8 ) 3 K 3 Li 3 (AlF 2 ) 3 in equal molecules. All the variations may be 
 accounted for by admixtures of muscovite, with sometimes a trivial 
 amount of the magnesium or iron salt, No. 6, as an impurity. 
 
 For purposes of illustration, four of the lepidolite analyses may be 
 considered in detail, as follows: E, from Rozena, by Berwerth, 1 F, 
 
 Juschakova, by Rammelsberg; 2 G, Schuttenhofen, by Scharizer; 3 H, 
 white lepidolite from Norway, Maine, by Riggs. 4 
 
 . 
 
 E. 
 
 F. 
 
 Gr. 
 
 1 
 
 H. 
 
 Si0 2 ------------ 
 
 50. 98 
 
 50. 96 
 
 49. 26 
 
 49. 52 
 
 ai 2 o 3 
 
 27. 80 
 
 22.20 
 
 25. 26 
 
 28. 80 
 
 Fe 2 0 3 
 
 .40 
 
 Mn 2 0 3 
 
 
 5. 38 
 
 
 
 MnO 
 
 
 .85 
 
 .07 
 
 .24 
 
 FeO 
 
 .05 
 
 
 .84 
 
 MgO 
 
 
 . 02 
 
 CaO 
 
 
 
 
 . 13 
 
 k 2 o 
 
 10. 78 
 
 11. 39 
 
 13.85 
 
 12. 63 
 . 13 
 
 ;Na 2 0 
 
 .32 
 
 .35 
 
 T.i.O 
 
 5.88 
 
 5.65 
 
 5.38 
 
 3.87 
 
 h 2 o 
 
 .96 
 
 1.76 
 
 1. 72 
 
 F 
 
 7. 88 
 
 8.58 
 
 5.68 
 
 5.18 
 
 p 2 Og 
 
 .05 
 
 SnO. 
 
 
 .06 
 
 
 
 
 
 
 Less 0 
 
 104. 38 
 3. 32 
 
 104.48 
 3. 61 
 
 103. 29 
 2. 38 
 
 102. 71 
 2. 18 
 
 
 
 101.06 
 
 100. 87 
 
 100. 91 
 
 100. 53 
 
 Disregarding trivial impurities, and computing the ratios as before, 
 we have from these analyses the subjoined empirical expressions: 
 
 E. Al347K230l<i392Hi06(AlF2)207(Si3O8)l8l(SiO 4 )306. 
 
 F . A1.28oK252Li376( AlF2)22fi(Si308) 212(Si04)2l2. 
 
 G. Al 3 45R ,/ 24K25oLi358Hi 96 ( AIF 2 ) 149( Si 3 Os) I ,%( Si04) 3 53« 
 
 H . A1434R' / 7K272Li 2 68Hi92( A1F 2 ) 136 ( S^Os) 141 ( SiO 4 )403* 
 
 Condensing, these become: 
 
 E. Al34 7 R / 935X 4 87. 
 
 F. Al28oR / 854X 4 24. 
 
 G. Al345R // 24R / 95sX509. 
 
 H. A1 4 34R // 7R / 858X544. 
 
 1 See Tschermak’s paper, 1. c. 
 
 2 Wiedemann’s Annalen, vol. 7, p. 143. 
 
 ! Zeitschr. Rryst., vol. 13, p. 467. 
 A Am. Jour. Sci., Nov. 1886. 
 
CLARKE.] 
 
 A THEORY OF THE MICA GROUP. 
 
 15 
 
 Whence we get, very nearly: 
 
 E. 70 AlX 3 R' 9 +92 A1 3 X 3 R ' 3 
 
 F. 71 AlX 3 R' 9 +70 A1 3 X 3 R' 3 . 
 
 G. 8 AlX 3 R" 3 R' 3 +75 AlX 3 R / 9 -f-87 AUXjjRV 
 
 H. 2 AlXaR'^RV^ A1X 3 R' 9 +127 AlaXaR's. 
 
 Two other highly fluoriferous lithia micas, cryophyllite and zinn- 
 waldite, may properly be considered here. For the former we have 
 Riggs’s analysis, and for the latter, analyses by Berwerth and Rammels- 
 berg. From these analyses we get the following empirical formula: 
 1, Riggs, cryophyllite; 2 and 3, Berwerth and Rammelsberg, zinn- 
 waldite. 
 
 1. Ali86Fe // 94K256Ui3-24H] 4 6(AlF 2 )i78;(Si 3 08)227(Si04)l85. 
 
 2. Al. 2 39Fe // i 8 6K236Li2i 8 H I 02(AlF 2 ) 20y (Si 3 O 8 ) l 5 1 (SiO4)3i2. 
 
 3. A1 244 F Q 1 * ifjj K 2 12 U 224 Uj ] 6 ( A1F 2 )20o( 8i 3 0s)l56( SiO4) 3 06» 
 
 Condensiug these formula they become : 
 
 1. Al 1 86Fe 94 R , 904X 4 i 2 . 
 
 2. Al 239 Fei86R / 765X 4 63* 
 
 3. Ah-HFe^R^saX^z. 
 
 Expanding again, these formulse give : 
 
 1. 31 (AlX 3 Fe // 3 R / 3 )+81(AlX 3 R / 9 )+25(Al 3 X 3 R / 3 ). 
 
 2. 62 “ +49 “ +43 
 
 3. 56 “ +53 “ +45 “ 
 
 The component molecules here correspond essentially to Nos. 6, 3, 
 and 1 of the fundamental series, the last one in each expression being 
 muscovite. Whether the separate components of R' and X can be 
 distributed with certainty among the several molecules is an outstand- 
 ing question; but not, I believe, an unanswerable one. 
 
 PHLOGOPITE. 
 
 In order to ascertain the composition of this mica I have discussed 
 the four analyses cited by Tschermak (1. c.), and three of Rammels- 
 berg’s. 1 All of these are fluoriferous, and all but one are phengitic, the 
 exception in the latter case being the Edwards, N. Y., mineral, which 
 Tschermak regards as somewhat altered. I have also considered the 
 new phlogopite from Edwards, recently described by Penfield, 2 which 
 is remarkable as being free from fluorine. 
 
 In general, phlogopite agrees closely with the formula AlX 3 Mg 3 B / 3 , 
 but there are often variations which are not easy to explain, and which 
 are greater than can be accounted for by presumable errors of analysis. 
 They may be due in part to impurities arising from the great altera- 
 bility of the mineral; but I am inclined to trace the difficulties toother 
 sources. 
 
 1 Wiedemann’s Annalen, vol. 9, p. 129. 2 Am. Jour. Sci. (3), vol. 36, p. 329. 
 
16 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 64. 
 
 In order to satisfy the conditions of the formulae proposed by me, it 
 is necessary that the aluminum atoms, apart from A1F 2 , shall be in 
 number at least one- third of X ; but in several phlogopites the alum- 
 ina is too low to fulfill this requirement, and the difficulty is best 
 obviated by assuming an MgF group in place of A1F 2 . In Penfield’s 
 phlogopite, however, there is no fluorine, and yet the alumina is con- 
 siderably — about two per cent- — too low. If we suppose in his mineral, 
 which came from a talc mine, a small admixture of talc, the residue 
 agrees with the theoretical formula, X being wholly Si0 4 ; but if that 
 impurity is absent we must assume that the mica differs from ordinary 
 phlogopite by containing the group — Mg — OH instead of the usual 
 MgF. The composition of the mineral then reduces to the uniform 
 type. I am now disposed to believe that phlogopite differs from the 
 other micas in that it contains these special groups MgF and MgOH, 
 both as part of R' ; but the supposition is not yet fully justified. It is, 
 however, I think, susceptible of experimental investigation, and a lab- 
 oratory research upon the problem is now being carried out under my 
 direction. Apart from that, the supposition is strengthened by the 
 composition of certain vermiculites, some of which have certainly been 
 formed by the alteration of phlogopite. Three of these interesting 
 minerals are represented fairly well by the subjoined formulse, in which 
 
 ferric iron, present in 
 alumina. 
 
 small quantities, has 
 
 been reckoned with the 
 
 Si0 4 — (MgOH) 3 Si0 4 — ) 
 
 Si0 4 — MgH 
 
 / 
 
 / >Mg 3 
 
 / 
 
 A1 — Si0 4 — A1 
 
 A1 — Si0 4 — S 
 
 Al — Si0 4 -MgH 
 
 \ 
 
 \ 
 
 \ 
 
 Si0 4 = AI 
 
 Si0 4 = A1 
 
 Si0 4 = Al 
 
 -j-3H 2 0. 
 
 +3H 2 0. 
 
 +3H 2 0. 
 
 Dudleyite. 
 
 Culsageeite. 
 
 Jefferisite. 
 
 It is by no means certain that the vermiculites are so simple in compo- 
 sition or so definite as these symbols would seem to indicate ; but the 
 formulae are decidedly suggestive, and they show how clearly the 
 relations between the micas and their derivatives may be expressed. 
 
 THE FERRO-MAGNESIAN MICAS. 
 
 This group of micas, which includes biotite, lepidomelane, annite, 
 haughtonite, siderophyllite, and other supposed species, is apparently 
 quite complex. In place of magnesia, ferrous iron is often predominant ; 
 in the lepidomelanes, ferric iron replaces aluminum, and in forty-four 
 out of the fifty-six analyses discussed, the oxygen was in excess of 
 Si0 4 . Only seven of these micas appeared to be phengitic ; and ohly 
 sixteen of the analyses reported fluorine in small quantities. In six 
 instances AlO and A1F 2 , were both absent. 
 
 For thirty-four of the micas in this group, formulae could be easily 
 computed upon the lines already followed ; that is, in each case the 
 
CLARKJE.J 
 
 A THEORY OF THE MICA GROUP. 
 
 17 
 
 composition was represented by a mixture of AlXgE'^E'g with AIXsE'g 
 and AI3X3R/3, the second or third of these molecules being occasionally 
 absent. Among the lepidomelanes there was an approximation to a 
 distinctively muscovitic type ; and in two cases formula No. 4, A1 3 X 3 E"E, 
 seemed to apply. With each mica an attempt was made to determine 
 the proportions of the several admixed molecules ; but the results, 
 although numerically conformable to the general theory, were not abso- 
 lutely conclusive. The chief difficulty lay in the uncertainty attaching 
 to the water determinations, upon which the question of oxygen excesses 
 depends. Since water has a low molecular weight, a small error in its 
 estimation becomes relatively large in the molecular ratios, and two 
 sorts of errors are presumable: First, an excess of water may be 
 inclosed mechanically in the material analyzed, and secondly, a deter- 
 mination by simple ignition is likely to be too low because of the oxida- 
 tion of ferrous iron. If these errors occur together, they obviously 
 tend to compensate each other ; but either one alone seriously affects 
 the co-efficient of E', and appears in the ratio between A1 3 X 3 E' 3 and 
 A 1 X 3 E' 9 . 
 
 In twenty-two of the fifty-six analyses, however, the symbol 
 AD^E^E^ failed to account for all the bivalent metals, iron and mag- 
 nesium. In these cases E" was in excess of E', and it became necessary 
 to make use of formula Xo. 7, Al 2 (Si0 4 )6E /, 9. With the aid of this 
 expression all the ferro-magnesian micas, without a positive exception, 
 including the phlogopites, were resolvable into mixtures of A1 3 X 3 E , 3 , 
 AlXgE'g, and AbXcE'V Upon this basis formula Xo. 6 becomes useless, 
 for •Al^X 3 ]VIg 3 E / 3 is evidently equivalent to a mixture, in equal molecules, 
 of AlXgE'g and Al 2 X 6 Mg 9 . Ail micas, th en, so far as the analyses are 
 authentic, may be represented as mixtures of the molecules 1, 3, and 
 7, these being symbols of one and the same general type. The magne- 
 sium (or ferrous) salt thus assumed, moreover, is not absolutely hypo- 
 thetical; for, with six molecules of water of crystallization added, it 
 approximates to certain individuals of the chlorite group. Some exam- 
 ples of penninite, for instance, approach rather closely to the composi- 
 tion Al 2 (Si0 4 ) 6 Mgg . 6H 2 0, which requires 38.71 of silica, 10.97 alumina, 
 38.71 magnesia, and 11.61 water. We have thus a clue to the constitu- 
 tion of the chlorites, by means of which they may be brought into 
 simple relation with the micas. This problem is now under investigation, 
 and I can only state as a probability that most of the chlorites, if not 
 all, may be represented as mixtures of three fundamental molecules, 
 A1 2 X6E" 9 , 6H 2 0 ; A1X 3 E" 3 H 3 , 3H 2 0, and Al 2 X 3 (MgOH) fi . I hope to 
 speak more positively upon this subject before long; at present I need 
 only point out that two of these molecules are simple hydrates of Xos. 
 6 and 7, while the third is covered by the general symbol Xo. 3, in which 
 E'g becomes (MgOH) 6 . The easy alterability of garnet, Al 2 (Si0 4 ) 3 E // 3 
 into mica and chlorite, is a suggestive bit of evidence bearing upon 
 these expressions. 
 
 Bull. 64 2 
 
18 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 61- 
 
 MARGARITE. 
 
 Whether this species is to be considered as a true mica or not, is 
 perhaps an open question. Its composition is relatively simple, and is 
 represented by the empirical formula H 2 CaAl 4 Si 2 Oi 2 . Structurally, this 
 may be written in two distinct ways, as follows: 
 
 OH Si0 4 E(A10) 2 H. 
 
 / _ / 
 
 Al — Si0 4 — CaH or Ca 
 
 ^SiO.E (AlO), >V Si0 4 E(A10) 2 H. 
 
 The first of these symbols derives the compound from the normal 
 aluminum salt, and indicates a similarity of type with the micas proper. 
 The second assumes a normal calcium salt as the point of derivation j 
 and I am unable as yet to assign a distinct preference to either ex- 
 pression. A careful study of the genesis and associations of margarite 
 may determine which of the two formulae is the better. Possibly the 
 occurrence of the mineral in such mixtures as euphyllite, and the 
 probable existence of a similar barium salt in cellacherite points to the 
 first of the two formulae as the better. The common occurrence of 
 margarite with diaspore also points in the same direction. Corundophi- 
 lite, which occurs associated with both margarite and diaspore, also 
 reduces to a type resembling the first margarite formula. 
 
 THE CLINTONITE GROUP. 
 
 These minerals, the so-called u brittle micas,” have also been discussed 
 by Tschermak, 1 who includes under this heading seybertite, brandisite, 
 xanthophyllite, ehloritoid, masonite, ottrelite, sismondine, and sapphir- 
 ine. Physically, they are closely related to the micas proper, and to 
 margarite in particular ; but chemically they are much more basic. The 
 first three species Tschermak regards as mixtures of the hypothetical 
 compounds H 2 CaMg 4 Si 3 0i 2 and H 2 CaMgAl 6 Oi 2 ; to ehloritoid he assigns 
 the composition H 2 Si 2 Fe // 2 0 7 , x H 2 A1 4 0 7 , and sapphirine he represents 
 by the formula Si 2 Mg 2 0 6 -bAl 6 Mg 2 O n . 
 
 Using the analyses cited by Tschermak, I find that all these minerals, 
 with the possible exception of sapphirine, may be represented by the 
 general expression 
 
 O 
 
 / >R" 
 
 Al-0 
 
 \ 
 
 Si0 4 = 
 
 R' 3 , 
 
 which is clearly and directly related to the formulae already assigned 
 to the micas and to margarite, and in which the mode of union of R u 
 with Al, when R"r=Mg, suggests the common association of mem- 
 bers of this group with spinel. In seybertite we have a mixture of 
 
 ' 1 Zeitsckr. Kryst., vol. 3, p. 496. 
 
CLABKE.] 
 
 A THEORY OF THE MICA GROUP. 
 
 19 
 
 A10 2 R"Si0 4 (Mg0H) 3 with Ai0 2 R"Si0 4 ( A10) 3 , R" being partly Oa and 
 partly Mg. In brandisite we have a similar constitution, with about one- 
 fourth of R" replaced by H 2 . In chloritoid, R"=Fe and R / 3 =H 2 (A10) ; 
 and sismondine is similar, with R' 3 possibly replaced in part by Al. The 
 compound A10 2 MgSi0 4 (A10) 3 , found in seybertite, is a rough approxi- 
 mation to sapphirine, which mineral possibly has this composition plus 
 some impurities as yet unidentified. A wider range of analyses is 
 needed in order to establish these formulae completely; but they seem 
 to have distinct advantages over the formulae proposed by Tschermak. 
 
 CONCLUSIONS. 
 
 All the micas, vermiculites, chlorites, margarite, and the ciintonite 
 group may be simply represented as isomorphous mixtures, every con- 
 stituent being a substitution derivative of normal aluminum polysilicate 
 or orthosilicate. To the latter compound a structure may be assigned 
 somewhat different in form from the one I have chosen, without affect- 
 ing in any notable way the general system adopted. Upon this basis 
 all the minerals named are reducible to the same general type, which 
 accounts for observed isomorphisms, and for the relations of the micas 
 to other species, with fewer assumptions of hypothetical compounds 
 than are necessary under other known schemes of interpretation. In 
 most cases the evidence is clear, direct, and conclusive ; in other cases, 
 few in number, it is at present somewhat obscure. It may be claimed, 
 without extravagance, that the formulae have the merit of suggestive- 
 ness, and that they form a scientific basis for future research. 
 
A PLATINIFEROUS NICKEL ORE FROM CANADA 
 
 By F. W. Clarke and Charles Catlett. 
 
 During the autumn of 1888 we received, through two different chan- 
 nels, samples of nickel ores taken from the mines of the Canadian 
 Copper Company at Sudbury, Ontario. From one source we obtained 
 two masses of sulphides, to be examined for nickel and copper ; from 
 the other source came similar sulphides, together with a series of soil 
 and gravel-like material, seven samples in all. In the latter case an 
 examination for platinum was requested, and in five of the samples it 
 was found, the gravel above mentioned yielding 74.85 ounces of metals 
 of the platinum group to the ton of 2,000 pounds. At the outset of 
 the investigation we were decidedly incredulous as to the existence of 
 platinum in such ores; but the discovery of sperrylite by Mr. Wells 
 in material from the same mines gave our work a wholesome stimulus, 
 and the assays were carefully carried through. 
 
 The sulphide ores submitted to us from Sudbury were all of similar 
 character. They consisted of mixed masses, in which a gray readily 
 tarnishing substance was predominant, with some chalcopyrite, possibly 
 some pyrite, and a very little quartz. Two samples were examined in 
 mass ; one gave 31.41 per cent of nickel with a little copper, the other 
 gave 35.39 per cent of nickel and 5.20 of copper. The nickel mineral 
 itself proved to be a suphide of nickel and iron, and as ores of that 
 composition are not common, it was thought desirable to examine the 
 substance further. 
 
 As above stated, the nickel mineral is the predominating constituent 
 of the masses submitted for examination. It is steel gray, massive, and 
 exceedingly alterable in the air, and its specific gravity, determined by 
 jjycnometer, is 4.541. An analysis of carefully selected material gave 
 the following results : 
 
 Ni.. 
 
 Fe.. 
 
 Si0 2 
 
 Cu.. 
 
 S... 
 
 41.96 
 15. 57 
 1.0*2 
 .62 
 40. 80 
 
 99.97 
 
 Neither cobalt nor arsenic could be detected. 
 
 The foregoing figures work out sharply into the ratio R : S : : 4 : 5 ; and 
 approximately into the formula Ni 3 FeS 5 . If we deduct silica, together 
 
 20 
 
C catlett! P ] NICKEL ORE FROM CANADA. 21 
 
 with the copper reckoned as admixed chalcopyrite, and recalculate the 
 remainder of the analysis to 100 per cent, we have the following figures : 
 
 
 As found. 
 
 Calc, as 
 Xi 3 FeS s . 
 
 m 
 
 j 43. 18 
 
 44.6 
 
 Fe 
 
 ! 15.47 
 
 14.4 
 
 S 
 
 41.35 
 
 41.0 
 
 
 100. 00 
 
 100.0 
 
 In short, the mineral has the composition Ni 4 S 5 , with about one-fourth 
 of the nickel replaced by iron. The only known species with which this 
 agrees is Laspeyres’s polydymite, of which the Sudbury mineral is evi- 
 dently a ferriferous variety. What relations it may bear toward bey- 
 richite, pyrrhotite, etc., is as yet a matter of considerable uncertainty. 
 Probably in most cases the nickeliferous constituent of pyrrhotite is 
 millerite, but other sulphides, like the polydymite, may perhaps occur 
 also. 
 
 The polydymite which was selected for the above analysis came from 
 the mass in which, in average, 35.39 Ni and 5.20 Cu had previously been 
 found. The mass weighed several kilograms, and was remarkably free 
 from quartz. The same mass, with two smaller pieces resembling it, 
 were also examined for platinum, by the following method : One assay 
 ton of the finely ground ore was treated with nitric acid until all or 
 practically all of the sulphides had been dissolved. The dried residue 
 was then assayed in the usual manner : except that, to facilitate cu- 
 pellation, a little pure silver was introduced into the lead button. From 
 the final bead the silver was dissolved out by sulphuric acid, leaving 
 the platinum in a finely divided gray powder. The latter dissolved 
 easily in aqua regia, and gave all the reactions needful to identify it 
 thoroughly. The results were as follows, “A” representing the large 
 mass in which the polydymite was determined : 
 
 Per cent. 
 
 A, 2.55 ounces Pt to the ton, or 0.0087 
 
 B, 1.8 ounces Pt to the ton, or 0060 
 
 C, 7 ounces Pt to the ton, or 0240 
 
 That the metal weighed was nearly all platinum is certain ; but it 
 may have contained small amounts of other metals of the same group. 
 The material separated was not sufficient to warrant a search for the 
 rarer associates of platinum. Probably the platinum exists in the ore 
 as sperrylite, although this point was not proved. The amount of plati- 
 num in the mass most thoroughly examined would require, to form 
 sperrylite, only about 0.007 per cent of arsenic, which is too small a 
 quantity for detection by ordinary analysis. That platinum should 
 exist in appreciable quantities in an ore of such character is something 
 quite extraordinary. Whether it could be profitably extracted is an 
 open question. 
 
A NEW OCCURRENCE OF GYROLITE. 
 
 By F. W. Clarke. 
 
 In the autumn of 1888, during a visit to the New Almaden Quick- 
 silver Mine in California, Dr. D. T. Day, of the U. S. Geological Survey, 
 was shown specimens of a mineral which was locally supposed to be 
 white fluor-spar. It occurred in well- developed crystals lining crevice 
 veins in the mine, and was easily recognizable as apophyllite. Dr. 
 Day secured a good series of the specimens, and finally turned them 
 over to me for examination. The largest crystals were about two 
 centimeters in diameter, and fairly transparent, and grew out of crys- 
 talline masses of considerable thickness, the exposed definite faces 
 nearly meeting at the center of the seam or vein. All of the specimens 
 were saturated with bituminous matter, but except for that staining 
 they were quite colorless. 
 
 In several of the specimens received the wall of the seam was dis- 
 tinctly shown, and between it and the crystalline apophyllite there was 
 a fibrous layer from one to three centimeters in thickness. That layer 
 was also colorless, except for bituminous staining, and on account of its 
 relations to the apophyllite it appeared to deserve investigation. A 
 sufficient quantity of the material having been selected, it was digested 
 for about twenty-four hours with ether in order to cleanse it from bitu- 
 men, and then analyzed. I give the result in comparison with How’s 
 figures for a Nova Scotia gyrolite : 
 
 
 Clarke. 
 
 How. 
 
 h 2 o 
 
 14.60 
 
 15.05 
 
 Si0 2 
 
 52.54 
 
 51. 90 
 
 A1 2 0 3 
 
 1. 27 
 
 Fe 2 0 3 
 
 j 0.71 
 
 CaO 
 
 29. 97 
 
 29. 95 
 
 MpO 
 
 0. 08 
 
 k 2 o 
 
 1.56 
 
 1.60 
 
 Xa 2 0 
 
 0. 27 
 
 F 
 
 0. 65 
 
 
 
 
 Less O 
 
 100. 30 
 0. 27 
 
 99. 85 
 
 
 
 
 100.03 
 
 
 
 
 22 
 
23 
 
 clarke.] A NEW OCCURRENCE OF GYROLITE. 
 
 It will at once be seen that the two analyses, except for the small 
 amount of fluorine, coincide quite sharply, and establish the New Alma- 
 den mineral as gyrolite. The Nova Scotian gyrolite is also associated 
 with apophyllite, from which species How supposed it to be derived. 1 
 In the present instance, however, the relative position of the two min- 
 erals in the vein suggests that the gyrolite is the older ; and that the 
 apophyllite may have been formed from it by a partial solution and 
 redeposition of its material through the agency of waters containing 
 alkaline fluorides. The gyrolite is obviously not absolutely pure, but 
 it agrees approximately with the formula Ca 2 Si 3 0 8 . 3H 2 0. Its chemi- 
 cal structure and relations to apophyllite are not altogether clear. 
 
 1 Am. Jour. Sci, (2), vol. 32, p. 13. 
 
ANALYSES OF THREE DESCLOIZITES FROM NEW LOCALITIES. 
 
 By W. F. Hillebrand. 
 
 1. MAYFLOWER MINE, BALD MOUNTAIN MINING DISTRICT, BEAVER- 
 HEAD COUNTY, MONT. 
 
 Through Messrs. W. H. Beck and George E. Lemon, of Washington, 
 D. 0., was received about a year ago for examination a large lump of 
 friable, un crystallized material, having a dull yellow to pale orange 
 color, and consisting chiefly of a vanadate, but carrying a large per- 
 centage of gangue. Two samples as pure as could be selected from 
 different parts of the lump were analyzed with the following results: 
 
 e ‘ 
 
 I. 
 
 II. 
 
 Mean. 
 
 Molecular ratios. 
 
 PbO 
 
 56. 02 
 
 55. 84 
 
 55. 93 
 
 . 2508 ^ 
 
 CuO 
 
 1.16 
 
 1. 13 
 
 1.15 
 
 . 0145 1 
 
 
 
 
 
 > . 4718 4. 02 
 
 FeO 
 
 0. 70 
 
 0.70 
 
 0. 70 
 
 .0097| 
 
 ZnO 
 
 15. 96 
 
 15. 91 
 
 15.94 
 
 . 1968 J 
 
 V 2 0 6 
 
 
 20. 80 
 
 20.80 
 
 
 As 2 0 5 
 
 0. 32 
 
 
 0. 32 
 
 . 1140 1 
 
 .0014 >.1173 1.00 
 
 P 2 0 6 
 
 0. 27 
 
 
 0. 27 
 
 . 0019 J 
 
 H 2 0 
 
 4. 37 
 
 4. 36 
 
 4. 37 
 
 . 2428 2. 07 
 
 Si0 2 ............ 
 
 0. 20 
 
 0. 16 
 
 0. 18 
 
 
 CaO 
 
 0. 10 
 
 
 0. 10 
 
 
 MgO 
 
 0. 06 
 
 
 0.06 
 
 
 
 
 
 99. 82 
 
 
 From I 27.62 per cent of gangue insoluble in cold dilute nitric acid 
 has been deducted, and from II 22.20 per cent ; manganese was pres- 
 ent in the gangue in small quantity, apparently as pyrolusite, but it 
 was not dissolved by the acid. The insoluble portion was found also 
 to retain very small quantities of lead and zinc, which were estimated 
 and included in the analysis as probably belonging to the vanadate. 
 The water had to be estimated indirectly by deducting from the total 
 amount of water afforded by the dried mixture of vanadate and gangue 
 that belonged to the latter alone, which was found as follows : The 
 mixture, dried at 100° C., was dissolved in cold dilute nitric acid, and 
 the insoluble matter collected in a Gooch crucible was dried at the same 
 temperature and then ignited. The loss on ignition gave the water in 
 24 
 
HILDEBRAND. ] 
 
 ANALYSES OF THREE DESCLOIZITES. 
 
 25 
 
 the gangue, there being no ferrous iron in the latter to influence the 
 result. The traces of Si0 2 , CaO, and MgO may be neglected as proba- 
 bly derived from the gangue. The water, it will be noticed, is double 
 that required by descloizite, R 2 (0H)V0 4 , but in view of the liability to 
 error inherent in the method of water estimation employed, this is not 
 deemed sufficient cause for separating the mineral from descloizite, 
 although the close agreement of the two water determinations, made 
 as they were on samples containing different proportions of gangue, 
 would indicate the correctness of the formula 2[R 2 (0H)V0 4 ] + H 2 0. 
 
 Other specimens have since been received from the above-named 
 persons in which the earthy vanadate was associated sometimes with 
 compact cerussite and galena in process of alteration. A dull reddish 
 substance which constituted a part or even the whole of some lumps 
 contained, besides silica, iron and some antimony in an oxidized condi- 
 tion, but carried little or no vanadium. 
 
 Prof. F. A. Genth has already called attention 1 to the occurrence of 
 vanadinite and probably of descloizite in the Bald Mountain mine, 
 Beaverhead County, Mont. His specimens, however, showed the sup- 
 posed descloizite as a pale brownish crystalline coating on yellow 
 ferruginous quartz, whereas the present mineral shows no evidence of 
 crystalline structure. 
 
 2. COMMERCIAL MINE, GEORGETOWN, GRANT COUNTY, N. MEX. 
 
 This is one of the most interesting occurrences of descloizite known, 
 because of the extreme brilliancy of coloring of the mineral. The ore 
 bodies in the Commercial mine, as well as in the adjoining MacGregor 
 and Naiad Queen mines, occur in limestone immediately under an over- 
 lying slate, and appear to narrow in depth where certain eruptive dikes 
 cut through the lime, as Mr. Macintosh, foreman of the Commercial 
 mine, informed me. The absence of the superintendents of the several 
 mines and the very brief visit I was forced to make prevented obtain- 
 ing more certain and detailed information. 
 
 In places where the rock is most fractured and crushed the descloi- 
 zite appears in greatest quantity and finest condition as an incrusta- 
 tion on quartz, often covering large surfaces, and in color varying from 
 yellow through all shades of orange-red to deep reddish brown, the 
 last-named colors predominating. The black color so frequent in 
 descloizite from Lake Valley, N. Mex., caused by a superficial coat- 
 ing or admixture of pyrolusite, is, so far as my observation extended, 
 wanting, hence specimens from Georgetown are likely to be much 
 sought after for their showy appearance. A specimen in one of the 
 banks at Silver City, N. Mex., taken from one of the Georgetown 
 mines, resembled a stalactite in form. It was probably fully three feet 
 in height by six to eight inches or more in diameter, and was deep 
 reddish brown in color. 
 
 1 Proc. Am. Phil. Soc., 1887, vol. 24, p. 38. 
 
26 
 
 WASHINGTON LABORATORY. 
 
 [bull. 64. 
 
 The incrustations are for the greater part distinctly crystalline and 
 are generally made up of aggregates of more or less globular forms of 
 a size ranging from microscopic to a diameter of one or two millimeters. 
 Each of these is composed of a great number of apparently flat crystals, 
 intergrown, and projecting sufficiently from the surface to give brilliant 
 reflections when observed under the lens, and to the naked eye a frosted 
 appearance where the globular growths are largest. The richest reddish 
 brown color is always coincident with this development in size. The 
 globular character changes frequently to acicular. In such cases the 
 incrustation seems to have originally formed on bunches of radiating 
 acicular, almost colorless, vanadinite, which frequently appears thus 
 coating the quartz and running under the descloizite incrustations. 
 Sometimes the vanadinite has entirely disappeared, and then there may 
 be a hollow through the center of the descloizite needle. 
 
 The occurrence of vanadate of lead in the MacGregor mine at 
 Georgetown has been noticed by Professor Genth (1. c., p. 38). The specific 
 gravity of the mineral was not determined ; the hardness is about 3.5; 
 the color of the powder is orange-yellow. An analysis gave the follow- 
 ing results after deducting 11.91 per cent of insoluble matter, almost 
 entirely quartz : 
 
 
 
 Molecular ratios. 
 
 PbO 
 
 CuO 
 
 FeO 
 
 ZnO 
 
 v 2 0 6 
 
 A 8205 
 
 p 2 0 6 
 
 h 2 o 
 
 Cl 
 
 Si0 2 
 
 CaO 
 
 MgO 
 
 56.01 
 1.05 
 0.07 
 17.73 
 20.44 
 0. 94 
 0. 26 
 2. 45 
 
 0. 04 
 
 1. 01 
 0. 04 
 0. 03 
 
 100.07 
 
 . 2512 , 
 
 . 0132 
 
 > . 4843 .4788 4.12 
 .0010 [ 
 
 .21891 
 
 .11191 
 
 .0041 !>. 1178 .1162 1.00 
 .0018] 
 
 . 1361 1361 1. 17 
 
 .0011 
 
 The third column of molecular ratios gives those values after allow- 
 ing for admixed vanadinite calculated on the basis of the chlorine 
 found. A further correction has probably to be made for an admixed 
 soluble hydrous (zinc ?) silicate, which might make the ratio approxi- 
 mate more closely to 4 : 1 : 1. 
 
 % 
 
 3. LUCKY CUSS MINE, TOMBSTONE, COCHISE COUNTY, ARIZ. 
 
 Mr. W. F. Staunton, superintendent of the Tombstone Mining and 
 Milling Company, and Mr. Frank C. Earle, assay er at Tombstone, 
 kindly placed at my disposal for examination specimens of a vanadium 
 mineral the identity of which had not been established. It was found 
 
IIILLEBRAXD.] 
 
 ANALYSES OF THREE DESCLOIZITES. 
 
 27 
 
 in the Lucky Cuss mine as an incrustation, sometimes half an inch 
 thick, on quartz, showing more or less botryoidal surfaces of an inde- 
 finable dull greenish color. On a fractured surface the color is brown ; 
 the luster is resinous ; the structure granular, only occasionally diverg- 
 ing fibrous ; the hardness 3.5 ; the specific gravity of sample analyzed 
 containing a little impurity, 5.88 at 19° C.; color of powder lemon- 
 yellow. Analysis gave the following results after deducting 0.67 per 
 cent of insoluble matter : 
 
 
 
 Molecular ratios. 
 
 PbO 
 
 CuO 
 
 FeO 
 
 ZnO 
 
 v 2 o 5 
 
 A8 2 0s 
 
 p 2 0 6 
 
 h 2 o 
 
 Cl 
 
 Si0 2 
 
 CaO 
 
 MgO 
 
 K 2 0 
 
 Na 2 0 
 
 C0 2 
 
 57.00 j 
 11. 21 
 Trace. 
 4. 19 
 19. 79 
 1.10 
 | 0.19 
 
 2. 50 
 0.07 
 0.80 
 1. 01 
 0. 04 
 0.10 
 0. 17 
 0. 82 
 
 98. 99 
 
 . 2556 1 
 . 1412 
 
 J* . 4485 .4385 3.93 
 
 . 0517 i 
 . 1084 ) 
 
 .0048 >.1145 .1115 1.00 
 . 0013 j 
 
 . 1389 1389 1. 25 
 
 .0020 
 
 The low total is probably owing to a loss of zinc during analysis. 
 Calcite was present as an impurity, and as the C0 2 just suffices for the 
 CaO and MgO these are rejected in considering the composition of the 
 vanadate. The figures in the third column of molecular ratios are 
 found by allowing for probably admixed vanadinite calculated from the 
 chlorine found. In another specimen a qualitative test for chlorine 
 indicated a greater admixture of vanadinite. As in the case of the 
 descloizite from Georgetown, N. Mex., previously described, a further 
 allowance has perhaps to be made for a soluble hydrous silicate. There 
 can be no doubt that the general formula for the vanadate is that of 
 descloizite. 
 
 In almost every respect this mineral resembles, so far as the published 
 descriptions allow of judging, the descloizite of Penfield, 1 the .cupro- 
 descloizite of Rammelsberg, 2 and the ramirite of de Leon, 3 perhaps 
 also the tritochorite of Frenzel, 4 to the similarity of which with his 
 variety of descloizite Penfield draws attention in his paper. Professor 
 Genth’s surmise (1. c., p. 39) of the specific identity of all these sub- 
 
 1 Am. Jour. Sci. (3), vol. 26, p. 361. 
 
 * 2 Monatsb. Berl. Acad., 1883, p. 1215. 
 
 3 La Rarairita, nueva espdcie mineral, Mexico, 1885. 
 
 4 Tschermak , s Min. and Petr. Mitth., vol. 3, p. 506, 1880, vol. 4, p. 97, 1881. 
 
28 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 64 . 
 
 stances seems highly probable. Characteristic of the present variety 
 is the greater replacement of the lead-zinc vanadate — truedescloizite — 
 by the isomorphous lead-copper vanadate and the lessened tendency 
 toward a fibrous structure, which in the other varieties described seems 
 to be a decidedly pronounced feature. Possibly this last characteristic 
 of the Tombstone mineral, if it be not accidental in view of the few 
 specimens (three) examined, is a condition of the first. 
 
 According to Rammelsberg, 1 the lead-copper vanadate corresponding 
 to the lead-zinc vanadate (descloizite) is mottramite or psittacinite, 
 though it seems not improbable that it may be the chileite of Dana’s 
 Mineralogy. Domeyko’s analyses, 2 which led Kenngott to ascribe the 
 above name to the Chilian mineral, show a deficiency of 2.5 and 2.8 per 
 cent, which may very well be V 2 0 5 . At all events, a recalculation of 
 his analyses based on this assumption leads to a proportion for 
 PbO-f CuO : V 2 0 5 : H 2 0 of nearly 4:1:1. 
 
 In view of the well defined character of all these highly cupriferous 
 varieties of descloizite it would be well to designate them once for all 
 by some distinctive name. Tritochorite would have precedence if the 
 substance to which that name has been given is really identical with 
 the others, but Rammelsberg’s cupro-descloizite is more appropriate as 
 indicating at once the relationship to descloizite, and I would suggest 
 that it be heneefortlf used for all cupriferous descloizites showing the 
 physical characteristics of the mineral above described. 
 
 Note. — Since the foregoing was written there has appeared in the 
 Bull. Soc. Franc. Min., Feb., 1889, p. 38, a paper by F. Pisani, in which 
 he gives another analysis of the Mexican cupro-descloizite and discusses 
 briefly the relations of various vanadates. The essential identity of 
 all the above-enumerated cupriferous lead-zinc vanadates, with the 
 addition of another — scliaffnerite, concerning which I have been unable 
 to find any further reference in mineralogical literature — is therein 
 upheld, and the suggestion of Penfield regarding the possible identity 
 of tritoshorite and cupro-descloizite is confirmed by Frenzel himself, 
 who is quoted as writing to Professor DesCloizeaux that he had not 
 thought it necessary to consider as an essential constituent the two 
 per cent of water which he had found in tritochorite. 
 
 1 Chemische Natur der Mineralien, p. 32. 
 
 2 Ann. d. Mines, IV, vol. 14, 1848, p. 150; Phil. Mag., Ill, vol. 34, 1849^ p. 395. 
 
A NEW METEORITE FROM MEXICO. 
 
 By J. Edward Whitfield. 
 
 While in Mexico during the summer of 1888, Prof. H. A. Ward, of 
 Ward and Howell, Rochester, 1ST. Y., obtained an undescribed mass of 
 meteoric iron weighing 33.0 kilos. 
 
 The meteorite was found on a peak of the Sierra de San Francisco, 
 called La Bella Roca, in front of Santiago Papasquiaro, in the State of 
 Durango. The date of its discovery and the name of the finder are 
 uuknown. 
 
 The composition of the metallic portion does not differ materially from 
 that of other meteoric irons, as the following analysis will show : 
 
 Fe 91.48 
 
 Ni ' 7.92 
 
 Co 0.22 
 
 P 0.21 
 
 S 0. 21 
 
 C 0.06 
 
 100. 10 
 
 • A feature of the meteorite is the presence of large, deep pittings on 
 one side $ these are a little greater in diameter just below than imme- 
 diately at the surface and each one has a little substance left at the 
 bottom, which evidently is the remains of what originally filled the 
 cavities. I succeeded in breaking from the bottom of one pitting 
 material sufficient to determine its nature. It proved to be troilite as 
 the analysis will show : 
 
 NiS2.13, FeS 85.27, Fe 9.37. • 
 
 The exposed surface of the troilite was greatly decomposed; this 
 portion gave by analysis the following figures : 
 
 NiS 2.07, FeS 37.51, Fe,0 3 37.60. Moisture, 19.85. 
 
 This decomposition gives grounds for the idea that the deep pittings 
 were formed by the removal of troilite nodules, partly while the mass 
 was hot and partly by the subsequent weathering. 
 
30 
 
 WASHINGTON LABORATORY. 
 
 [bull, 64 . 
 
 There are nodules of troilite throughout the entire mass of the 
 meteorite, but none are removed so. as to form pittings, on any other part 
 of the surface but the side which is supposed to have been forward. 
 
 The mass is deeply furrowed and all the furrows tend away from the 
 side containing the pittings. 
 
 Slices of the meteorite, when etched, show rather coarse Widman- 
 stattian figures and also dark diagonal bands of troilite. 
 
 From the locality in which this meteorite was found it is but proper 
 that it should be called u La Bella Boca.” 
 
 I am indebted to Messrs. Ward and Howell for the material for ex- 
 amination and the privilege of description. 
 
DUMORTIERITE FROM HARLEM, N. Y., AND CLIP, ARIZ. 
 
 By J. S. Diller and J. E. Whitfield. 
 
 In 1887 Dr. R. B. Riggs published a description, including a chemical 
 analysis, of u the so-called Harlem iudicolite,” which was regarded as 
 probably a new boro-silicate. The notice led to correspondence with 
 Prof. E. S. Dana, who identified the mineral as dumortierite, and kindly 
 sent us some of the original dumortierite from near Lyons, France, for 
 comparison. 
 
 The physical properties of the Harlem dumortierite agree very closely 
 with those mentioned by Bertrand, 1 Gonnard, 2 and Darnour. 3 Crystals 
 are very rare. An imperfect one 4 has been observed with a( coPoo ) and 
 m{ ocP) equally developed. Both planes are striated parallel to the 
 vertical axis. Indistinct reflections allowed only approximate meas- 
 urement am= 152°, and therefore mm =124°. Obtuse terminal planes 
 rarely observed on embedded crystals. 
 
 Cleavage parallel to a is distinctly developed so that when the min- 
 eral is crushed and examined under a microscope cleavage plates may 
 be found which show an obtuse bisectrix lying parallel to b( ooPoo ). 
 Cross fractures occasionally yield basal sections which may be made 
 to exhibit an acute bisectrix. Extinction always takes place parallel 
 to the vertical axis and the mineral is evidently rhombic. 5 In cross- 
 sections imperfect cleavage is rarejy seen parallel to some prismatic 
 plane. Polysynthetic twinning is very common parallel to b as well as 
 to other planes in the prism zone. Liquid inclusions and long tubular 
 cavities parallel to the vertical axis are abundant. Hardness =7 and 
 specific gravity slightly above 3.265. 
 
 The rock in which the dumortierite occurs at Harlem is the pegmatoid 
 
 1 Bull. Soc. Min. d. France, vol. 3, 1880, p. 171, and vol. 4, 1881, p. 9. 
 
 2 Bull. Soc. Min. d. France, vol. 3, 1881, p. 2. 
 
 3 Bull. Soc. Min. d. France, vol. 4, 1881, p. 6. 
 
 4 It was kindly loaned to us by Mr. R. T. Chamberlin, of New York. Our thanks 
 are also due to Mr. George F. Kunz for the material he so generously furnished for 
 this investigation. It was collected along Fourth avenue at One hundred and twen- 
 tieth and One hundred and twenty-second streets, as well as near Fort George, a new 
 locality of the same district. 
 
 b My observations, noted in Mr. Riggs’s paper, already referred to, were very hastily 
 made with imperfect apparatus, and published before I had an opportunity for their 
 
 revision. — J. S. Dillek, 
 
 31 
 
32 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 64 , 
 
 portion of a biotite gneiss. These coarse vein-like parts are composed 
 of quartz with both red and colorless orthoclase, some plagioclase and 
 tourmaline. The other portions of the rock contain much biotite and 
 garnet. The fibers of dumortierite are sparingly scattered through the 
 quartz in the coarse granular rock. A few were observed penetrating 
 plagioclase. The thin, thread-like fibers are occasionally so small as 
 not to be distinctly dichroic, but they are intermingled and connected 
 with larger dichroic fibers by every intermediate gradation in size, so 
 that an observer at once regards them all as the same mineral. They 
 sometimes closely resemble the trichitic forms in granitic quartz, which 
 Dr. G. W. Hawes 1 and many others following his suggestion regarded 
 as rutile. 
 
 The presence of tourmaline in the rock at Harlem was not at first 
 recognized. It is so intimately associated with the dumortierite that 
 they can not be easily separated. Their pleochroic phenomena, however, 
 are so unlike that they can be readily distinguished under a polarizing 
 microscope. The presence of tourmaline renders the results of Mr. 
 Riggs’s analysis less trustworthy. By means of the Klein solution and 
 an electro magnet the tourmaline was separated from the dumortierite. 
 The .217 gram of the latter thus obtained was analyzed with the fol- 
 lowing result. 2 Only the smallest trace of B 2 0 3 was observed. 
 
 SiO-2 31.44 A1 2 0 3 68.91 
 
 Fortunately, at the time it became particularly desirable to obtain a 
 larger quantity of dumortierite for analysis a collection of minerals was 
 sent by Mrs. 0. A. Bid well from Clip, Yuma County, Arizona, to the 
 National Museum for identification. Among them Prof. F. W. Clarke 
 noticed a blue mineral, which proved to be dumortierite. It is finely 
 fibrous and so abundant as to give color to the rock, which is composed 
 chiefly of granular quartz. A few grains of magnetite and limonite 
 are the only other minerals intermingled with the quartz and dumorti- 
 erite, so that it seems an easy matter by means of a heavy solution and 
 an electro-magnet to obtain the latter mineral for chemical analysis. 
 The results are given under I, below. 
 
 These figures appear to show the material analyzed to be impure, and 
 it was thought advisable to obtain more of the rock and endeavor to 
 separate the dumortierite as far as practicable from all impurities. 
 Mrs. C. A. Bid well kindly furnished a sufficient amount of much better 
 material, in which the only mineral associated with the dumortierite 
 was quartz. As dumortierite is not acted upon by hydrofluoric acid ; 
 the rock, after being crushed to small particles, was digested in this acid 
 for a length of time sufficient to decompose most of the quartz. The 
 mass was then washed with water, dried, and any quartz that might 
 still remain separated by Thoulet’s solution. After thorough washing 
 
 1 Mineralogy and Lithology of N. H., 1878, p. 45. 
 
 2 The chemical work for this paper was done by Mr. Whitfield. 
 
•whSfVl™] dumortierite. 33 
 
 the material was examined with the aid of a microscope and found to 
 be free from gangue. Having been ground exceedingly fine and dried 
 at 104° C. for about three hours, the mineral was analyzed with the fol- 
 lowing results (II) : 
 
 
 I. 
 
 II. 
 
 Si 2 0 2 ....... 
 
 31. 52 ‘ 
 
 27.99 
 
 A1 2 0 3 
 
 63. 66 
 
 64. 49 
 
 CaO 
 
 trace. 
 
 * 
 
 MgO 
 
 .52 
 
 trace. 
 
 Na 2 0 
 
 .37 
 
 
 K 2 0 
 
 .11 
 
 
 b 2 o 3 
 
 2. 62 
 
 4. 95-4. 93 
 
 p 2 o 5 
 
 
 0. 20 
 
 Ignition 
 
 1.34 
 
 H 2 0 1.72 
 
 
 100. 14 
 
 99. 35 
 
 Analysis II shows less impurity than the first specimen analyzed. 
 These results indicate either that dumortierite is not a simple silicate 
 of aluminum as stated by Damour; 1 or else that the material analyzed 
 was a mixture of dumortierite with some other compound. 
 
 If we assume the formula of Damour to be correct and estimate all 
 the Si0 2 in the analysis as belonging to the formula Al 8 Si 3 0 18 , then 
 there will be left unaccounted for a small amount of A1 2 0 3 , H 2 0, and 
 B 2 G 3 , and these are present in the proportions represented by the for- 
 mula A1B 3 0 6 . 2H 2 Q. If this mode of interpretation be correct, then 
 the mineral from Arizona corresponds approximately to the formula 
 3Al 8 Si 3 0] 8 .AlB 3 0 6 . 2H 2 0 which requires Al 2 0 3 =65.2 percent; Si(J 2 ==27.6 
 per cent; B 2 0 3 =5.4 per cent; H 2 Q=1.S per cent, agreeing quite 
 closely with the actual analysis. A borate of aluminum corresponding 
 to the above formula is, we believe, not actually known, and concerning 
 its properties nothing can be predicted. If it exists it is certainly re- 
 markable that it should withstand the treatment with hydrofluoric acid 
 which the dumortierite received during the process of purification. 
 
 We are greatly indebted to Mrs. C. A. Bidwell for the supply of 
 material for investigation, which at the cost of much personal labor she 
 so liberally furnished. 
 
 1 Ball. Soc. Min. de France, vol. 4, p. 6. 
 
 Bull. 64 3 
 
CHEMICAL ACTION BETWEEN SOLIDS.' 
 
 By William Hallock. 
 
 In a note on a new method of forming alloys published some time 
 ago, 1 2 1 suggested some additional experiments which I intended to 
 make, and I now give the results thus far obtained. Unfortunately, 
 other work prevents my continuing the investigation at present. 
 
 Inasmuch as the method and principle 3 seemed well established 
 where metals were used to produce alloys, an attempt was made to 
 include some chemical reactions in the list. The most natural cases 
 were the freezing mixtures where solid reagents are used. In order to 
 surely have both constituents in a decidedly solid state the experiments 
 were performed in a vessel cooled to a temperature of minus 10° or 12° 
 C., care being always taken to leave the reagents in the vessel long 
 enough for them to assume a temperature decidedly below zero Centi- 
 grade. Under these conditions a crystal of rock salt (NaCl) and a piece 
 of clean, dry ice were gently brought in contact, lying side by side on 
 a watch glass. Of course the result was the solution of salt, but old 
 as this experiment may be, it appears here in a new connection, as an 
 example of the union of two solids below the melting point of either, 
 but above that of the product. The piece of ice was frozen to the 
 glass and during the operation the crystal was drawn several millime- 
 ters across the glass, doubtless by capillarity, as the solution ran out 
 at the bottom of the surface of contact as fast as it formed, the attrac- 
 tion being sufficient to move a crystal several grams in weight. 
 
 Similar experiments were performed with sodium and potassium, 
 nitrate potassium, calcium and ammonium chloride, and sodium and 
 potassium hydrate, with a similar result in all cases. These are all well 
 known results, but wherein do they differ from the new method of form- 
 ing alloys % This question suggests another. Are the metals combin- 
 ing to form an alloy in the new way a freezing mixture ? A thorough 
 
 1 This paper was read in part before the Phil. Soc. of Washington, D. C., October 
 13, 1888, and appeared in full in the Am. Jour. Sci., vol. 37, 1889, p. 402. 
 
 2 W. Hallock, Zeitschr. f. Phys. Chem., vol. 2, 1888, p. 6. Science, vol. 11, 1888, p. 
 
 265. 
 
 3 O. Lehmann, Wiedemann Ann., vol. 24, 1885, p. 5, suggested the theoretical pos- 
 sibility of producing an alloy in this way. I had overlooked his paper until recently. 
 Mr. Lehmann, however, evidently did not consider it possible to fulfill the necessary' 
 conditions and did not try the experiment. 
 
 34 
 
HALLOCK.] 
 
 CHEMICAL ACTION BETWEEN SOLIDS. 
 
 35 
 
 investigation of the question would require more complicated experi- 
 ments than I had time to perform. One test, however, is very simple, 
 that with potassium and sodium. 
 
 Into a small porcelain crucible weighing 15 grams and containing 
 about an equal weight of petroleum were placed pieces of the two 
 metals, about 3 grams of each. One junction of a thermo-element 
 was forced into the piece of potassium and gave its temperature accu- 
 rately. After the whole had assumed the room temperature, clean 
 faces of the two metals were brought into contact^ the liquefaction began, 
 and the temperature immediately fell . It required about two hours to 
 complete the liquefaction and about one and a half hours to attain the 
 minimum of temperature. No precautions were taken to prevent the 
 calorimeter taking up heat from its surroundings, and, no doubt, it 
 absorbed considerable in the long time, aud yet the maximum fall in 
 temperature amounted to 2.4° C., very large, considering the small 
 weight of the reagents compared with the calorimeter. Thus it appears 
 that sodium and potassium are, under such circumstances, a u freezing 
 mixture,” and analogy at least would lead one to believe that other 
 alloys also absorb heat in their formation; but future experiment must 
 decide the point. 
 
 In the cool vessel above described a piece of sodium or potassium was 
 placed upon a piece of dry ice; almost instantly the reaction commenced 
 and proceeded vigorously. It is, however, scarcely safe to consider 
 this a case of chemical action between solids, because the reaction is 
 probably as follows: The vapor from the ice attacks the metal, forming 
 the hydrate which unites with other ice, forming a solution, which is 
 then further acted upon by the metal, and in the whole process heat is 
 generated sufficient to raise the temperature of the reagents very con- 
 siderably. Perhaps in the other freezing mixtures, ice and salt, etc., it 
 is the vapor of the water or ice which initiates the reaction. 
 
 In view of these and other considerations, the idea is evident that 
 perhaps many substances have a slight vapor tension at temperatures 
 considerably below their melting points, and are surrounded by a thin 
 atmosphere of their own vapor over their clean surfaces, and it is only 
 necessary to bring two such atmospheres to interpenetration in order 
 to initiate the reaction which will then continue, provided the product 
 (liquid or gas) escapes easily and does not clog the operation. In very 
 many cases substances are found to give oft' a vapor below their melt- 
 ing point, and it is natural to suppose that there is a film of that vapor 
 over the surface of the body, as there is a layer of saturated air over 
 water. The mechanical theory of the composition of matter lends 
 plausibility to the above suggestion. If these considerations are correct 
 they foretell the regelation of substances like camphor and ice, without 
 any pressure whatever. That loose pieces of camphor will become 
 welded together by simple contact is well known. The operation 
 appears to me thus : In an irregular mass of camphor in an atmos- 
 
36 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 64 . 
 
 phere of camphor vapor, there is a constant interchange of state for the 
 molecules at the surfaces of the solid, molecules previously solid are 
 getting too far off and becoming gas, and molecules previously gas are 
 beating upon the solid and staying there ; thus the state of equilibrum 
 is when, as a whole, there are as many molecules which fly off and 
 become gas as fly on and become solid. On a projecting point of the 
 solid the chances are in favor of more flying off than on; in a reentrant 
 angle the reverse is true. Theoretically, then, the piece ought ultimately 
 to become a sphere, not only by the rounding down of the corners, 
 but by the building up of the flat or reentrant sides. That the corners 
 do round off all know. If this is all true we only need to bring the two 
 pieces together and consider them as one, and the crack between them 
 as a reentrant angle, and the union is brought about as above indi- 
 cated. If in the above the word liquid be substituted for vapor or gas, 
 the explanation will apply to the regelation of ice in water at 0° C. 
 
 We may go even further and predict a uniting without actual contact, 
 and this prediction has been experimentally demonstrated in the case 
 of ice and water. A large rough block of ice (about 15 pounds) was 
 sawed nearly in two, the slit washed out and all the fine pieces removed. 
 In this way it was possible to hold two plane surfaces of ice parallel 
 and near each other (1 t<T 2 mm ) without danger of actual contact. Into 
 the outer edge of the saw-cut a cotton wick was pressed, thus isolating 
 the space between the faces from the outside and preventing any cur- 
 rents from circulating through the crack. The whole block was then 
 placed in water at zero and inclosed in non-conducting cases and left 
 for twenty-five to thirty hours. This experiment was tried three times 
 and each time a freezing across the space had taken place. The whole 
 space was not filled, but in numerous places, notably along just inside 
 the wicking and up from the bottom of the cut. No doubt the regela- 
 tion would have gone further if the experiment could have been con- 
 tinued longer. The melting of the whole block puts an end to each 
 experiment. As these experiments were performed in summer there is 
 scarcely a possibility that the ice was colder than 0° 0. 
 
 Inasmuch as there appears to be an increasing inclination to regard 
 solutions and alloys as chemical compounds, it seems justifiable to speak 
 of the action according to the alloy law as chemical. On the other 
 hand, there are some cases which at first appear as chemical action 
 between solids which upon closer investigation can be explained on a 
 simpler assumption. 
 
 For example, Mr. W. Spring, 1 in a recent paper on this subject, cites 
 three particular cases as being chemical action between solids, the 
 union of copper and sulphur, the reaction between copper and mercuric 
 chloride, and between potassium nitrate and sodium acetate. 
 
 The formation of the sulphide of copper and other sulphides was ac- 
 complished by Mr. Spring by compression of the elements. But it is 
 
 1 W. Spring, Zeitschx. fur phys. Chemie, vol. 2, 1888, p. 536. 
 
HALLOCK.] 
 
 CHEMICAL ACTION BETWEEN SOLIDS. 
 
 37 
 
 not even necessary that the sulphur and copper be in contact. I have 
 made the sulphide at ordinary temperatures with the two an inch apart 
 and a wad of cotton in the tube between them. It is simply the vapor 
 of sulphur which attacks the copper. That sulphur gives off a per- 
 ceptible vapor at ordinary temperatures, especially in vacuo, is a fact 
 any one can easily demonstrate. The case of the copper and mercuric 
 chloride is precisely the same. The vapor of the chloride will go 
 through a whole tube past cotton wads and attack the copper, or color 
 potassic iodide. Hence we can scarcely assert that these reactions are 
 between solid bodies. The reaction between potassium nitrate and 
 sodium acetate is equally unconvincing. Mr. Spring expected an in- 
 terchange of bases and acids and left the mixture of the dry fine 
 powders four months in a desiccator to give time for the exchange. On 
 removing them from the desiccator a deliquescence was noticeable and 
 he therefore concludes that the interchange had taken place, since the 
 original salts do not easily deliquesce ; but the product of the reaction 
 (potassium acetate) does. It appears to me thus : The moment the 
 powders were brought to the air, the water vapor enters the operation 
 and we have potassium nitrate, water vapor, and sodium acetate, and 
 the result of their mutual interaction is a solution of potassium acetate 
 and sodium nitrate. In fact, if the dry powdered salts are stirred 
 together, in a very few moments deliquescence begins, showing that 
 whatever the reaction it goes on at once, and is a matter of moments 
 and not of months. Thus even this experiment in its present form 
 does not convince us that a chemical exchange took place before the 
 water vapor entered the reaction. 
 
 The question of chemical action between solids is by no means new, 
 but is being constantly extended. I may say I believe chemical action 
 may take place wherever the product or products are liquid or gaseous 
 even though the reagents are solid, with perhaps the added condition 
 that one or both the reagents be soluble in the liquid produced. If this 
 be true my new method of forming alloys is but a special case of the 
 above general principle . 1 
 
 1 Experiments endeavoring to produce carbon disulphide from the elements at 
 ordinary temperatures, are in hand and give promise of positive results. Also, ex- 
 periments on the interaction of potassium nitrate and sodium acetate have been 
 started ; it will, however, be some time before further results can be given. 
 
THE FLOW OF SOLIDS: A NOTE. 
 
 By William Hallock. 
 
 The American Journal of Science, vol. 34, 1887, p. 277, contained an 
 abstract of my paper under the above title, which appears in full in 
 Bulletin 55 of the U. S. Geological Survey. The results obtained were 
 so different from those of Mr. Spring that I was led to a criticism of his 
 work and seem to have been misunderstood. 1 
 
 The justice of Mr. Spring’s 2 protest against a part of my original 
 paper I am glad to admit, as far as it concerns an ill-advised use of 
 terms, and a consequent misrepresentation of his views, of course en- 
 tirely unintentional. Not realizing that many were not so familiar with 
 Mr. Spring’s works as myself, I neglected in the brief paper to give his 
 views, and thus my deductions from his results seemed to represent his 
 own conclusions. 
 
 The object of my original investigation 3 was a solution of the ques- 
 tion whether pre-sure alone is capable of producing true liquefaction ; 
 many have certainly believed so, or even do believe so, and a few, at 
 least, including myself, saw in Mr. Spring’s earlier results evidence of 
 such a possibility. I believe that to produce such phenomena, as some 
 recrystallizations, and diffusion, an increase in the freedom of motion of 
 the molecule, an increased diffusibility, i. e., the beginning of a lique- 
 faction, is indispensable. Hence i looked upon his results as pointing 
 to a liquefaction by pressure. My own experiments with the same sub- 
 stances and pressures showed the impossibility of liquefying them by 
 pressure and even brought out an enormous increase in the rigidity of 
 bees-wax and paraffin 4 under such pressures. In concluding I wished 
 only to call attention to the difference between Mr. Spring’s results and 
 my own, but unfortunately a loose and abbreviated quotation caused 
 the misunderstanding, which I wish to explain. 
 
 Since obtaining my own results there seems to me little doubt that 
 many, at least, of Mr. Spring’s effects are caused rather by a motion 
 
 1 The following appeared in Am. Jour. Sci., vol. 36, 1888, p. 60. 
 
 2 W. Spring, Am. Jour. Sci., vol. 35, 1888, p. 78, also Bull, de PAcad. R. Belg.,vol. 14, 
 1887, p. 585. 
 
 3 W. Hallock, Am. Jour. Sci., vol. 34, 1887, p. 277. 
 
 ‘‘Compare also Ordnance Department Tests of Metals, etc., 1884, Government Print- 
 ing Office, pp. 252-254, 285-287. 
 
 38 
 
HALLOCK.] 
 
 THE FLOW OF SOLIDS. 
 
 39 
 
 under pressure , a kneading, as it were, and by the regrinding. The 
 holders in which his compressions were made were not tight and the 
 most perfect welding 1 always took place at the surface of the block, or 
 the corners, or where the material was forced into the cracks, often 
 even while the center, under equal pressure, remained almost un- 
 affected. My holders were tight, allowing no leaking or motion, and 
 the substances showed scarcely a trace of a welding under pressure. 
 I must therefore reiterate that which I wished originally to impress, 
 namely, that the majority of Mr. Spring’s results are not produced by 
 simple cubic static pressure. 
 
 In the Cases of chemical action and the formation of alloys, I believe 
 that the motion under pressure will be found to be the all important 
 factor, perhaps just as stirring assists diffusion to completely mix two 
 liquids. Even if blocks of barium sulphate and of sodium carbonate 2 
 were brought into actual chemical contact, I think no one would expect 
 that simple diffusion would complete the interchange of bases and acids 
 in finite time so long as both substances remained solid 5 nor that a 
 piece of copper and of tin soldered together would diff use and form a 
 homogeneous bronze ; nor would they expect that simple cubic static 
 pressure would promote these reactions ; if pressure will assist them 
 to completion, it will increase the diffusibility of solids, increase the 
 freedom of motion of their molecules ; that is, it will make them more 
 like liquids — will begin to liquefy them. 
 
 I wish to refer here to a new law I recently proposed 3 concerning the 
 formation of alloys, where the fact is brought out that the melting 
 point and liquidity of the product are quite as important as those of the 
 constituents in determining the possibility of a reaction. Mr. Spring 4 
 has produced Wood’s alloy by compressing the constituents together, 
 and quotes Mr. Romna 5 as having failed to obtain fine platinum wire 
 by electro silver-plating a platinum wire, drawing it down and dissolv- 
 ing off the silver in nitric acid, because the silver and platinum alloyed 
 under the pressure of the draw plate. Messrs. W. & L. E. Gurley, of 
 Troy, 1?. Y., have for several years made fine platinum wires by the 
 well-known Wollaston 6 method of casting silver around the platinum and 
 treating as above. In the note referred to 4 I have described the pro- 
 duction of Wood’s alloy without pressure at 100 ° C. of a tin-lead alloy 
 at 190° C. of the sodium-potassium alloy at ordinary temperatures, etc. 
 Hence it appears to me that pressure alone is the least important factor 
 in the production of the effects obtained in Mr. Spring’s investigation. 
 
 1 W. Spring, Bull. d. PAcad. R. Belg. , vol. 49, 1880, p. 352. Phosphore amorphe et seq. 
 
 2 W. Spring, Bull. Soc. Chein., vol. 44, 1885, p. 166. 
 
 3 W. Hallock, Science, Mar. 2, 1888, vol. 11, p. 100; also Ostwald Zeitschr. f. Pliys. 
 Chem., vol. 2, 1888. 
 
 4 W. Spring, Ber. der deutsch. Chem. Gesell., vol. 15, 1882, p. 595. 
 
 6 Ibid. 
 
 6 Ganot’s Physics, Atkinson, New York, 1883, p. 76. 
 
MISCELLANEOUS ANALYSES. 
 
 1. TYROLITE . 1 
 
 From the Mammoth Mine, Tintic district, Utah. New material, very 
 pure, collected and analyzed by W. F. Hillebrand. 
 
 CuO 45.08 
 
 FeO .? r 08 
 
 CaO .' ... 6.78 
 
 MgO 04 
 
 H 2 0 17. 21 
 
 AS 2 O 5 ...... — . — ...... .... — . .... .... ... — - .... 28. 52 
 
 S0 3 2.23 
 
 Insoluble * 16 
 
 100. 10 
 
 2. GADOLINITE. 
 
 From Llano County, Texas. Analyzed by L. G. Eakins. 2 
 
 Si0 2 23.79 
 
 Th0 2 * 58 
 
 Fe 2 0 3 96 
 
 Ce 2 0 3 2.62 
 
 (DiLa) 2 0 3 5.22 
 
 (YEr) 2 0 3 41.55 
 
 FeO 12.42 
 
 GIO 11. 33 
 
 MnO trace 
 
 CaO 74 
 
 MgO trace 
 
 Alkalies trace 
 
 H 2 0 1. 03 
 
 P 2 0 6 05 
 
 100. 29 
 
 In the rare earths from this mineral the absorption spectrum of 
 didymium was strong, and that of erbium was weak. The molecular 
 weight of the oxide (YEr) 2 0 3 was 260. 
 
 1 Compare analyses in Bulletin 55, p. 41. 
 
 3 Compare Hidden & Mackintosh, Am. Jour. Sci., Dec., 1889. 
 40 
 
CfiATAKP.] 
 
 MISCELLANEOUS ANALYSES. 
 
 41 
 
 3. WARWICKITE. 
 
 From the well-known locality at Edenville, Orange County, New 
 York. Analyzed by J. E. Whitfield. The material could not be com- 
 pletely freed from an admixture of spinel. 
 
 Si 0 2 - 
 Ti0 2 . 
 FeO.. 
 AI2O3 
 
 b 2 o 3 . 
 
 CaO . 
 MgO. 
 HoO . 
 
 1.16 
 18. 68 
 14.23 
 9. 44 
 18. 96 
 .38 
 34.41 
 2. 80 
 
 100. 06 
 
 From this composition no simple formula can be deduced ; but if we 
 reject obvious impurities, and thro^out the alumina in the form of 
 spinel, the residue agrees approximately with the ratios 
 
 Ti0 2 . B 2 O 3 . 4R // 0. 
 
 This expression is not quite satisfactory, and may need revision. 
 
 4. MINERALS AND ROCKS FROM MARYLAND. 
 
 Collected by Dr. G. H. Williams. 
 
 Chrome tourmaline and fuclisite . — Found in chrome pits a mile west 
 of Etchison post-office, a little east of Great Seneca Creek, in Mont- 
 gomery County. The tourmaline occurs in dark-green needles, with 
 chromite, and the mica is associated with it. Analyses by T. M. Chat- 
 
 ard. 
 
 
 Tourmaline. 
 
 Fuchsite. 
 
 H 2 0 
 
 3. 74 
 
 6. 77 
 
 Si0 2 
 
 36. 57 
 
 42.21 
 
 ; b 2 o 3 
 
 8. 90 
 
 
 F 
 
 .06 
 
 
 P 2 Og 
 
 .04 • 
 
 
 Ti0 2 
 
 .09 
 
 
 A1 2 0 3 
 
 32. 58 
 
 34.55 
 
 Cr 2 0 3 
 
 4. 32 
 
 2. 03 
 
 Fe 2 0 3l FeO 
 
 .79 
 
 1.03 
 
 NiO 
 
 .05 
 
 
 MnO 
 
 trace 
 
 trace 
 
 CaO 
 
 .75 
 
 .47 
 
 MgO 
 
 9.47 
 
 3. 13 
 
 Li 2 0 
 
 trace 
 
 
 KajO 
 
 2. 22 
 
 .82 
 
 X 2 0 
 
 .13 
 
 •9. 16 
 
 
 99.71 
 
 100. 17 
 
42 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 64. 
 
 These minerals are more fully discussed by G. H. Williams and A. 
 C..Gill in Circular No. 75 of the Johns Hopkins University. In the 
 same paper is described epidote from the Woodstock granite, of which 
 the following analysis has been made by Dr. W. F. Hillebrand, on only 
 0.4473 gramme of material: 
 
 Si0 2 37.63 
 
 Fe 2 0 3 (+Fe0) 15.29 
 
 A1 2 0 3 18.40 
 
 Ti0 2 3.78 
 
 MnO 31 
 
 CaO 22.93 
 
 MgO 31 
 
 P 2 Os 44 
 
 Ignition 2. 23 
 
 101. 32 
 
 Rocks from Baltimore County . — Analyses by J. E. Whitfield. A, 
 pyroxenite, Johnny Cake Eoad. B, pyroxenite, Johnny Cake Eoad, 
 first stage of alteration. C, pyroxenite, Johnny Cake Eoad, second 
 stage of alteration. D, smaragdite, Dogwood Eoad. 
 
 ♦ 
 
 A. 
 
 B. 
 
 f 
 
 C. 
 
 1 
 
 D. 
 
 Si0 2 
 
 50. 80 
 
 50. 10 
 
 51. 94 
 
 53.22 
 
 S0 3 
 
 trace 
 
 trace 
 
 .19 
 
 trace 
 
 Cl 
 
 .24 
 
 .26 
 
 .16 
 
 .26 
 
 P 2 O s 
 
 trace 
 
 none 
 
 none 
 
 
 AI 2 O 3 — 
 
 3. 40 
 
 2 . 00 
 
 2.53 
 
 3. 14 
 
 Cr 2 0 3 ............. 
 
 .32 
 
 .36 
 
 .60 
 
 .23 
 
 Fe 2 0 3 ............. 
 
 1. 39 
 
 2. 38 
 
 2 . 88 
 
 trace 
 
 FeO 
 
 8.11 
 
 8 . 68 
 
 9. 38 
 
 7. 95 
 
 MnO 
 
 .17 
 
 .29 
 
 trace 
 
 .11 
 
 CaO 
 
 12. 31 
 
 5.06 
 
 3. 60 
 
 14. 44 
 
 MgO 
 
 22. 77 
 
 26. 85 
 
 25. 97 
 
 20. 09 
 
 Alkalies 
 
 traces 
 
 none 
 
 none 
 
 traces 
 
 H a O 
 
 .52 
 
 4. 16 
 
 2. 82 
 
 . 98 
 
 
 100. 03 
 
 100. 14 
 
 100. 07 
 
 100. 42 
 
 Titanium was absent from all four. 
 
CATLETT.] 
 
 MISCELLANEOUS ANALYSES. 
 
 43 
 
 Another pyroxenite (E), and a diallage-bronzite rock (F), from the 
 same region, were analyzed by T. M. Chatard. 
 
 
 E. 
 
 F. 
 
 Si0 2 
 
 43.87 
 
 53. 98 
 
 Ti0 2 
 
 .12 
 
 .15 
 
 p 2 o 6 
 
 trace 
 
 trace 
 
 A1 2 0 3 
 
 1.64 
 
 1. 32 
 
 Cr 2 0 3 . — ........... 
 
 .44 
 
 .53 
 
 Fe^ 
 
 8. 94 
 
 1. 41 
 
 FeO 
 
 2. 60 
 
 3. 90 
 
 MnO 
 
 .19 
 
 .21 
 
 NiO 
 
 trace 
 
 trace 
 
 CaO 
 
 6.29 
 
 15. 47 
 
 MgO 
 
 27. 32 
 
 22. 59 
 
 Alkalies ( AsNa 2 0) . . 
 
 .50 
 
 undet. 
 
 H 2 0 
 
 8. 72 
 
 .92 
 
 
 100. 63 
 
 100. 48 
 
 5. SERPENTINE AND ITS ASSOCIATES. 
 
 From Moriah , New York . — Derived from pyroxene. Four analyses by 
 Charles Catlett, as follows : A, serpentine from the ophiolite of Feed’s 
 Quarry. B, “dolomite” from the same rock. C, pyroxene from an 
 abandoned quarry. D, serpentine derived from the same pyroxene. 
 
 
 A. 
 
 B. 
 
 C. 
 
 D. 
 
 Si0 2 
 
 39. 96 
 
 2. 60 
 
 55. 36 
 
 42.17 
 
 A1 2 0 3 ......... 
 
 1. 07 
 
 .09 
 
 .22 
 
 .30 
 
 Fe 2 0 3 
 
 3.53 
 
 none 
 
 .18 
 
 1.57 
 
 FeO 
 
 3. 85 
 
 .80 
 
 .57 
 
 .64 
 
 MgO 
 
 37. 61 
 
 2. 49 
 
 19. 53 
 
 41.33 
 
 CaO 
 
 none 
 
 52. 38 
 
 24. 48 
 
 none 
 
 C0 2 
 
 none 
 
 41. 77 
 
 none 
 
 MnO 
 
 trace 
 
 .04 
 
 trace 
 
 trace 
 
 H 2 0 
 
 13. 65 
 
 13.72 
 
 
 
 
 
 99. 67 
 
 100. 17 
 
 100. 34 
 
 99. 73 
 
 Chromium and nickel sought for, but absent. 
 
 Serpentine from the aqueduct shaft , New York City . — Analyzed by Mr. 
 
 Catlett : 
 
 Si0 2 . 39.92 
 
 AL0 3 08 
 
 Fe 2 0 3 50 
 
 FeO none 
 
 MgO 42.52 
 
 C0 2 1. G4 
 
 CaO 90 
 
 H 2 0 at 105° 1.36 
 
 Ignition... 13.26 
 
44 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 64. 
 
 From Montville , New Jersey. — A, very pale serpentine, somewhat re- 
 sembling deweylite in appearance. B, mineral, resembling actinolite. C, 
 brown mica, first zone above pyroxene. D, yellowish mica, second zone 
 above the pyroxene. E, white mica, associated with pyroxene. Analy- 
 ses A and B, by L. G. Eakins ; C, D, and E, by Charles Catlett. In D 
 and E the ferrous oxide was not separately estimated for want of suf- 
 ficient material. 
 
 Associates of serpentine from Easton , Pennsylvania. — A, vermiculite, 
 analyzed by C. Catlett; B, tremolite; C, so-called “nephrite.” Analy- 
 ses B and C by L. G. Eakins. 
 
 
 A. 
 
 B. 
 
 C. 
 
 Si0 2 
 
 42. 21 
 
 58. 27 
 
 60. 29 
 
 A1 2 0 3 
 
 9.37 
 
 .33 
 
 20. 83 
 
 Fe 2 03 
 
 .68 
 
 trace 
 
 trace 
 
 FeO 
 
 none 
 
 
 
 MnO 
 
 none 
 
 .08 
 
 
 CaO 
 
 none 
 
 11. 90 
 
 . 16 
 
 MgO 
 
 34. 80 
 
 25.93 
 
 6. 44 
 
 Na 2 0 
 
 1. 25 
 
 1. 25 
 
 1.97 
 
 k 2 o 
 
 1.34 
 
 .42 
 
 8. 41 
 
 H 2 0 
 
 10.70 
 
 1.22 
 
 1.13 
 
 
 100. 35 
 
 99. 40 
 
 99. 23 
 
 All of the foregoing minerals were collected by Mr. G. P. Merrill. 
 
 
 A. 
 
 B. 
 
 C. 
 
 H 2 0 
 
 14. 73 
 
 1. 17 
 
 5.07 
 
 C0 2 
 
 1 .30 
 
 Si0 2 
 
 40. 64 
 
 43. 31 
 
 39. 38 
 
 A1 2 0 3 . 
 
 2. 74 
 
 17.41 
 
 15. 92 
 
 Fe 2 0 3 
 
 .81 
 
 .71 
 
 .71, 
 
 .80$ 
 
 FeO 
 
 .28 
 
 . 59 
 
 MnO 
 
 trace 
 
 . 14 
 
 trace 
 
 CaO 
 
 trace 
 
 12.84 
 
 .28 
 
 MgO 
 
 40.93 
 
 19. 39 
 
 26. 85 
 
 Na 2 0 
 
 2.23 
 
 .62 
 
 K 2 0 
 
 
 1. 36 
 
 9. 84 
 
 F 
 
 
 .62 
 
 
 
 
 Less O.. 
 
 100. 13 
 
 99. 15 
 
 100. 39 
 . 26 
 
 
 
 
 
 
 
 100.13 
 
 D. 
 
 E. 
 
 10. 88 
 
 10. 20 
 
 1. 80 
 
 
 32. 52 
 
 39. 14 
 
 18. 14 
 
 15. 70 
 
 2.30 
 
 1.68 
 
 trace 
 
 trace 
 
 1. 44 
 
 5. 24 
 
 29.26 
 
 25. 44 
 
 1. 38 
 
 .64 
 
 2. 78 
 
 2.06 
 
 
 
 10C. 50 
 
 100. 10 
 
CHATARD.] 
 
 MISCELLANEOUS ANALYSES. 
 
 45 
 
 6. GEYSERITES FROM ROTORUA, NEW ZEALAND. 
 
 Received from the museum at Auckland. Analyzed by J. E. Whit- 
 field for comparison with the geyserites of the Yellowstone Park, which 
 they closely resemble. Three samples : 
 
 
 1. 
 
 2. 
 
 3. 
 
 Si0 2 
 
 92.47 
 
 90. 28 
 
 74. 63 
 
 A1 2 0 3 
 
 2. 54 
 
 3. 00 
 
 15. 59 
 
 CaO 
 
 .79 
 
 .44 
 
 1.00 
 
 MgO 
 
 • 15 ■ 
 
 trace 
 
 trace 
 
 Ha 2 0 
 
 .30 
 
 K 2 0 
 
 
 
 1. 02 
 
 Ignition 
 
 3. 99 
 
 6. 24 
 
 7.43 
 
 
 
 99.94 
 
 99. 96 
 
 99. 97 
 
 7. MISCELLANEOUS ROCKS. 
 
 Sandstone from Buena Vista , Ohio . — A yellowish building stone. Par- 
 tial analysis by F. W. Clarke. 
 
 Moisture 2.51 
 
 SiO-2 88.27 
 
 Al. 2 O 3 -fFe. 2 O 3 9.09 
 
 MgO trace 
 
 99. 87 
 
 Insoluble in HC1 96.47 
 
 Soluble FezOa 77 
 
 Sandstone from near Portsmouth , Ohio . — The “ Peebles-Henley 77 or 
 “Otway’ 7 building stone. Three samples, analyzed by T. M. Chatard. 
 In B and C the iron was mainly ferrous, though weighed as Fe 2 0 3 . 
 
 
 i A. 
 
 B. 
 
 C. 
 
 Ignition 
 
 1.08 
 
 1.46 
 
 1.95 
 
 Insoluble in HC1 
 
 98. 31 
 
 97. 20 
 
 95. 83 
 
 Soluble 
 
 .61 
 
 1.40 
 
 2. 42 
 
 . 
 
 100. 00 
 
 100. 06 
 
 100. 20 
 
 Soluble Fe^ 
 
 .61 
 
 i7oT 
 
 1.6 5~ 
 
 Soluble CaO 
 
 trace 
 
 .36 
 
 .77 
 
 ! Soluble MgO 
 
 trace 
 
 little 
 
 trace 
 
46 
 
 WASHINGTON LABORATORY. 
 
 [BULL. 64. 
 
 Limestone from Silverdale , Kansas. — Analyzed by Charles Catlett. 
 
 5. 27 
 1.07 
 .71 
 .32 
 50. 36 
 .56 
 .20 
 .10 
 40. 34 
 .07 
 .06 
 .78 
 
 99. 84 
 
 Metamorphic rock from Marion , Kentucky. — Analyzed by L. G. Eak- 
 
 34. 50 
 14. 37 
 2. 85 
 4.46 
 11.43 
 21.81 
 1.50 
 . 51 
 7. 14 
 .77 
 .60 
 .21 
 
 100. 15 
 
 From Pigeon Point , Michigan. — Analyses by L. G. Eakius. A, red por- 
 phyry from Brick Island, Lake Superior, near Pigeon Point. B, green 
 mottlings from Pigeon Point. Van Hise’s rock, No. 11908. 
 
 
 A. 
 
 B. 
 
 sl 0 2 — ....... 
 
 73.70 
 
 83.27 
 
 Ti0 2 
 
 .12 
 
 trace 
 
 AI 2 O 3 
 
 12. 87 
 
 7. 81 
 
 F 62 O 3 
 
 3. 76 
 
 1.99 
 
 FeO 
 
 .31 
 
 1. 81 
 
 MnO 
 
 .07 
 
 
 
 CaO 
 
 .14 
 
 .20 
 
 MgO 
 
 .11 
 
 1. 59 
 
 K 2 0 
 
 4. 56 
 
 1.11 
 
 Na 2 0 
 
 3.63 
 
 .19 
 
 H 2 0 
 
 .57 
 
 2. 32 
 
 P 2 O f 
 
 trace 
 
 trace 
 
 
 99. 84 
 
 100. 29 
 
 Si0 2 • - 
 A1 2 0 3 . 
 Fe 2 0 3 *. 
 FeO.. . 
 CaO .. 
 MgO. . 
 K 2 0. . 
 Na 2 0 . 
 
 h 2 o.. 
 
 F2O5 . . 
 
 S0 3 ... 
 
 co 2 ... 
 
 Si0 2 . 
 A1 2 0 3 
 Fe 2 0 3 
 FeO . 
 CaO. 
 MgO. 
 Na 2 0. 
 K 2 0 . 
 
 co 2 .. 
 
 so 3 .. 
 
 p 2 o 5 . 
 
 h 2 o. 
 
E AKINS.] 
 
 MISCELLANEOUS ANALYSES. 
 
 47 
 
 Diabase , Penokee- Gogebic Range , Michigan . — Analyses by. T. M. Cha- 
 tard. A, from near SE. corner of Sec. 13, T. 47 N., R.46 W. B, altered 
 diabase, same locality. 0, altered diabase, Aurora Mine, NE. J ot S W. 
 J Sec., T. 47 N., R. 47 W. D, feldspar separated from A. 
 
 
 A. 
 
 B. 
 
 C. 
 
 D. 
 
 H 2 0, at 105° 
 
 .15 
 
 3.12 
 
 .29 
 
 \ 1 1 Q 
 
 H 2 0, at red heat 
 
 2.34 
 
 8.25 
 
 13. 54 
 
 / i. 
 
 C0 2 
 
 .38 
 
 1.89 
 
 .38 
 
 1. 89 
 
 p 2 o 5 - 
 
 . 13 
 
 . 16 
 
 . 14 
 
 
 Si0 2 
 
 47. 90 
 
 46. 85 
 
 41.60 
 
 51.18 
 
 Ti0 2 
 
 .82 
 
 1. 12 
 
 3. 79 
 
 
 A1 2 0 3 
 
 15.60 
 
 22. 62 
 
 37. 20 
 
 27. 00 
 
 Fe 2 0 3 
 
 3.69 
 
 5.12 
 
 3.21 
 
 3. 19 
 
 Cr 2 0 3 
 
 trace 
 
 
 
 
 FeO 
 
 8. 41 
 
 1. 58 
 
 : 30 
 
 undet. 
 
 NiO 
 
 . 10 
 
 . 08 
 
 
 
 MnO 
 
 .17 
 
 2. 54 
 
 .08 
 
 .17 
 
 BaO 
 
 .05 
 
 . 10 
 
 trace 
 
 
 CaO 
 
 9. 99 
 
 1. 25 
 
 .23 
 
 11.70 
 
 MgO 
 
 8.11 
 
 2.01 
 
 .02 
 
 1. 92 
 
 k 2 o 
 
 .23 
 
 2. 66 
 
 
 .41 
 
 NajO 
 
 2. 05 
 
 .80 
 
 .07 
 
 3. 48 
 
 
 100. 12 
 
 100. 15 
 
 100. 85 
 
 100. 24 
 
 Penokee- Gogebic rocks from Wisconsin. — A, B, 0, three slates, analyzed 
 by L. G. Eakins. A, from Sec. 6, T. 45 N., R. 2 E. B, from Sec. 1, T. 
 45 N., R. 1 E. 0, from Sec. 4, T. 44 N., R. 2 W. 
 
 
 A. 
 
 B. 
 
 C. 
 
 Si0 2 .............. 
 
 53.44 
 
 59. 73 
 
 52. 58 
 
 A1 2 0 3 
 
 19. 62 
 
 22. 78 
 
 20. 76 
 
 Fe 2 0 3 
 
 11. 38 
 
 .11 
 
 12. 17 
 
 FeO 
 
 5. 35 
 
 5. 98 
 
 4. 08 
 
 MnO 
 
 trace 
 
 .09 
 
 .21 
 
 CaO 
 
 .42 
 
 .53 
 
 .30 
 
 MgO 
 
 1.58 
 
 2. 94 
 
 1. 33 
 
 K 2 0 
 
 1.73 
 
 3. 48 
 
 4. 87 
 
 NaiO 
 
 2. 61 
 
 1.41 
 
 .37 
 
 Li 2 0 
 
 trace 
 
 
 trace 
 
 H 2 0 
 
 4.07 
 
 3. 28 
 
 3. 43 
 
 P 2 O s 
 
 trace 
 
 
 
 
 100. 20 
 
 100. 33 
 
 100. 10 
 
48 
 
 WASHINGTON LABORATORY. 
 
 | BULL. 64. 
 
 D, E, F, three feldspars, analyzed by T. M. Chatard. D, from gabbro, 
 center of Sec. 14, T. 4£ N., R. 4 W. E, F, from olivine diabase, NE. J 
 Sec. 13, T. 45 N., R. 1 W. 
 
 
 D. 
 
 E. 
 
 F. 
 
 H 2 0, at 105° 
 
 .03 
 
 
 .13 
 
 H 2 O, at red lieat . . 
 
 .54 
 
 5 - 9o ! 
 
 .64 
 
 Si0 2 
 
 51.99 j 
 
 61. 65 
 
 56.15 
 
 ai 2 o 3 
 
 29.32 ! 
 
 19.91 
 
 26. 05 
 
 F e 2 0 3 — 
 
 1.23 j 
 
 2.28 
 
 1. 98 
 
 FeO 
 
 undet. ! 
 
 undet. 
 
 undet. 
 
 MnO 
 
 trace j 
 
 . trace 
 
 .13 
 
 CaO 
 
 12. GO i 
 
 4. 12 
 
 8.70 
 
 AT crO ..... 
 
 .63 1 
 
 .61 
 
 . 54 
 
 k 2 o 
 
 . 28 ; 
 
 5. 72 
 
 1. 56 
 
 Na^O 
 
 ! 2.91 ! 
 
 4. 74 
 
 i 4.79 
 
 
 j 99.53 
 
 99.98 
 
 100.67 
 
 Eruptive rock from four miles southwest of Hot Springs , Arkansas . — , 
 Analyzed by L. G. Eakins. 
 
 SiO, . 
 Ti0 2 . 
 
 ai 2 o 3 . 
 
 Fe 2 0 3 
 FeO . 
 CaO . 
 MgO. 
 K 2 0. 
 Na,0. 
 H 2 0 . 
 C0 2 . 
 P2O,. 
 
 36. 40 
 .42 
 12. 94 
 8.27 
 4.59 
 14. 46 
 11.44 
 3.01 
 .§7 
 2. 36 
 3. 94 
 1.04 
 
 99. 84 
 
 Recent lava from two miles south of Mount Trumbull , Arizona . — - 
 Analyzed by L. G. Eakins. 
 
 Si0 2 . 
 Ti0 2 . 
 A1 2 0 3 
 Fe 2 0 3 
 FeO . 
 M 11 O. 
 CaO. 
 MgO. 
 K 2 0 . 
 Na 2 0 
 H 2 0- 
 P2O,. 
 
 45. 30 
 2. 66 
 14.95 
 1.98 
 9.32 
 trace 
 8. 87 
 8.29 
 
 1.27 
 
 4.27 
 .85 
 
 2.23 
 
 99. 99 
 
Bakins.] MISCELLANEOUS ANALYSES. 49 
 
 Eruptive rock from Castle Mountain , Montana . — Analyzed by L. G. 
 
 Eakins. 
 
 Si0 2 44. 66 
 
 Ti0 2 1.02 
 
 A1 3 0 3 - 12.12 
 
 F 62O3 5.81 
 
 FeO 3.20 
 
 MnO 21 
 
 CaO 8. 14 
 
 MgO 8. 77 
 
 K 2 0 : 2.75 
 
 Na 2 0 - 4.47 
 
 H 2 0 4. 33 
 
 C0 2 2.19 
 
 P 2 0 5 2. 02 
 
 99. 69 
 
 Rocks from Northern California . — Collected by J. S. Diller. A, 
 porphyritic rocks from Shasta County; analyzed by J. E. Whitfield, 
 east fork of Clear Creek, nine miles from French Gulch. B, Smith’s 
 Gulch, six miles up Clear Creek from French Gulch. 
 
 
 A. 
 
 B. 
 
 Si0 2 
 
 66. 30 
 
 64.24 
 
 Ti0 2 
 
 trace 
 
 .76 
 
 S0 3 
 
 .28 
 
 .22 
 
 Cl 
 
 none 
 
 .25 
 
 P 2 O 5 
 
 .15 
 
 .08 
 
 ai 2 o 3 
 
 17.55 
 
 18. 67 
 
 F e 2 0 3 
 
 2.19 
 
 1.40 
 
 FeO 
 
 .55 
 
 1.96 
 
 MnO 
 
 trace 
 
 trace 
 
 CaO 
 
 3. 12 
 
 4.11 
 
 MgO 
 
 .97 
 
 1.48 
 
 NTa 2 0 
 
 5. 15 
 
 4. 14 
 
 k 2 o 
 
 2. 45 
 
 1.71 
 
 H 2 0 
 
 1.25 
 
 1.18 
 
 
 99. 96 
 
 100. 20 
 
 Bull. 64 4 
 
 W 
 
50 
 
 WASHINGTON LABORATORY. 
 
 (bull. 64. 
 
 C, D, two rocks from tliree-fourtks of a mile below John Allen’s, Dry 
 Creek, Shasta County. E, from John Allen’s. F, from two and one-half 
 miles above John Allen’s. Analyses by Whitfield. 
 
 G, eruptive rock, Great Bend of Pit River. H, black obsidian, Medi- 
 cine Lake, Modoc County; analyses by L. G. Eakins. 
 
 
 Gr. 
 
 H. 
 
 Si0 2 
 
 44. 77 
 
 73. 51 
 
 Ti0 2 
 
 . 53 
 
 
 p 2 0 6 . 
 
 .72 
 
 .04 
 
 A 1203 
 
 17. 82 
 
 14. 42 
 
 F e 2 0 3 ......... 
 
 5. 05 
 
 .46 ; 
 
 FeO 
 
 6. 95 
 
 1.49 | 
 
 M 11 O 
 
 trace 
 
 trace | 
 
 CaO 
 
 10. 36 
 
 1.26 | 
 
 MgO 
 
 8.22 
 
 .33 | 
 
 Na 2 0 
 
 2. 13 
 
 4.03 ! 
 
 K 2 0 
 
 .92 
 
 4. 29 
 
 H 2 0 
 
 2.64 
 
 .40 : 
 
 
 100. 11 
 
 100.23 j 
 
 
 C. 
 
 D. 
 
 E. 
 
 F. 
 
 Si0 2 .......... 
 
 59. 10 
 
 61. 60 
 
 54. 55 
 
 60.74 
 
 Ti0 2 
 
 .70 
 
 trace 
 
 trace 
 
 .86 
 
 S0 3 
 
 trace 
 
 .27 
 
 .10 
 
 .40 
 
 Cl 
 
 trace 
 
 trace 
 
 .12 
 
 trace 
 
 P 2 O 5 
 
 trace 
 
 .08 
 
 .10 
 
 trace 
 
 A1 2 0 3 
 
 14.02 
 
 12. 15 
 
 10.64 
 
 10.25 
 
 Fe 2 0 3 
 
 3. 16 
 
 2. 09 
 
 1.59 
 
 4.31 
 
 FeO 
 
 1.42 
 
 3. 30 
 
 1. 16 
 
 6.21 
 
 MnO 
 
 trace 
 
 trace 
 
 1. 53 
 
 trace j 
 
 CaO 
 
 9.35 
 
 6 . 92 
 
 14. 30 
 
 4.97 | 
 
 MgO 
 
 1. 72 
 
 2. 33 
 
 1.29 
 
 3.69 
 
 Na 2 0 
 
 2. 21 
 
 2. 16 
 
 2 . 60 
 
 1. 83 
 
 K 2 0 
 
 1.49 
 
 1.41 
 
 1.68 
 
 .52 
 
 C0 2 
 
 4. 65 
 
 5. 05 
 
 9. 05 
 
 2. 29 
 
 H 2 0 
 
 2. 63 
 
 3. 10 
 
 1. 60 
 
 4. 36 
 
 
 100. 45 
 
 100. 46 
 
 100. 31 
 
 100. 43 
 

 CATLETT.] 
 
 MISCELLANEOUS ANALYSES, 
 
 51 
 
 8. SOILS AND CLAYS. 
 
 A, kaolin from Talladega, Alabama. B, clay from Richfield Springs, 
 New York; partial analysis. C, D, two clays from Northumberland 
 County, Pennsylvania; analyses by Charles Catlett. 
 
 
 A. 
 
 B. 
 
 C. 
 
 D. 
 
 H 2 0, at 120° 
 
 H 2 0, at red heat 
 
 5.02 
 13. 48 
 
 00 
 
 to 
 
 | 6.28 
 
 j 6.87 
 
 Si0 2 
 
 43. 21 
 
 49. 65 
 
 65. 97 
 
 59. 16 
 
 Al 2 03 
 
 37.27 
 
 |23. 82 
 
 20.37 
 
 18. 68 
 
 F e 2 0 3 — .. 
 
 trace 
 
 2. 75 
 
 10. 32 
 
 CaO 
 
 .11 
 
 6. 48 
 
 .64 
 
 .52 
 
 MgO 
 
 .30 
 
 trace 
 
 .52 
 
 .67 
 
 K 2 0 
 
 .28 
 
 undet. 
 
 3. 32 
 
 3. 35 
 
 Na 2 0 
 
 .40 
 
 undet. 
 
 .05 
 
 .11 
 
 
 99. 87 
 
 96. 13 
 
 99. 90 
 
 99. €8 
 
 E, F, G, H, adobe soils. E, from Santa Fe, New Mexico. F, Fort 
 Wingate, New Mexico. G, Humboldt City, Nevada. H, Salt Lake 
 City, Utah. Analyses by L. G. Eakins. 
 
 
 E. 
 
 F. 
 
 G. 
 
 H. 
 
 Si0 2 ...... .......... 
 
 66. 69 
 
 26. 67 
 
 44. 64 
 
 19.24 
 
 A1 2 0 3 
 
 14. 16 
 
 .91 
 
 13.19 
 
 3. 26 
 
 Fe 2 0 3 
 
 4.38 
 
 .64 
 
 5. 12 
 
 1. 09 
 
 MnO 
 
 .09 
 
 trace 
 
 .13 
 
 trace 
 
 CaO 
 
 2. 49 
 
 36.40 
 
 13.91 
 
 38. 94 
 
 MgO 
 
 1. 28 
 
 .51 
 
 2. 96 
 
 2. 75 
 
 k 2 o 
 
 1. 21 
 
 trace 
 
 1. 71 
 
 trace 
 
 Na^ 
 
 .67 
 
 trace 
 
 . 59 
 
 trace 
 
 C0 2 
 
 .77 
 
 25. 84 
 
 8. 55 
 
 29. 57 
 
 p 2 o 6 
 
 .29 
 
 .75 
 
 .94 
 
 .23 
 
 S0 3 
 
 .41 
 
 .82 
 
 .'64 
 
 .53 
 
 Cl ? 
 
 .34 
 
 .07 
 
 .14 
 
 .11 
 
 h 2 o 
 
 4. 94 
 
 2. 26 
 
 3. 89 
 
 1.67 
 
 Organic matter 
 
 2.00 
 
 5. 10 
 
 3.43 
 
 2. 96 
 
 
 99. 72 
 
 99. 97 
 
 99. 84 
 
 100. 35 
 
 9. ORES OF IRON AND MANGANESE. 
 
 Manganese ore, Powell’s Fort, east end of Massanutten Mountain. 
 Warren County, Virginia. Analysis by Charles Catlett. 
 
 Si0 2 
 Fe.. 
 Mn . 
 P... 
 S... 
 
 9. 20 
 3. 07 
 48. .^9 
 .349 
 
 ,12 
 
52 
 
 WASHINGTON LABORATORY. 
 
 [bull. 61 
 
 Iron and manganese ores, Montebello, Nelson County, Yirginia. 
 Analyses by Catlett. 
 
 
 Iron. 
 
 Manganese. 
 
 Si0 2 
 
 16. 47 
 
 1.68 
 
 Fe 
 
 51. 10 
 
 2 . 60 
 
 Mn 
 
 .65 
 
 46. 99 
 
 P 
 
 .152 
 
 .464 
 
 S 
 
 .11 
 
 .21 
 
 Ores from Rockbridge County, Yirginia; analyzed by T. M. Chatard. 
 A, top of hill above Hart’s Bottom, one and three-fourths miles southwest 
 of Green Forest Station, near Lockland Station. B, Moorman Quarry, 
 Green Forest. C, new opening, No. 2, Buena Yista. D, opening, No. 3, 
 40-foot vein, Buena Yista. E, Chalk Mine Branch. F, Old Colonial 
 opening, Buena Yista. 
 
 
 A. 
 
 B. 
 
 C. 
 
 D. 
 
 E. 
 
 F. 
 
 H 2 0, 105° 
 
 .72 
 
 .15 
 
 .39 
 
 .60 
 
 .45 
 
 .48 
 
 Insoluble 
 
 20. 40 
 
 13.47 
 
 22.55 
 
 16. 60 
 
 8. 05 
 
 5. 43 
 
 Soluble AI 2 O 3 . - ■ 
 
 1. 67 
 
 
 .37 
 
 1 . 81 
 
 .46 
 
 
 Ti0 2 
 
 . 16 
 
 
 
 
 
 
 Fe 2 0 3 
 
 3.11 
 
 76. 19 
 
 66. 58 
 
 71. 16 
 
 78.24 
 
 82. 15 
 
 NiO 
 
 
 
 . 27 
 
 
 
 
 MnO 
 
 53.91 
 
 .45 
 
 .22 
 
 .11 
 
 .66 
 
 .19 
 
 BaO 
 
 .23 
 
 
 
 
 
 
 S0 3 
 
 .32 
 
 .14 
 
 .09 
 
 .37 
 
 trace 
 
 .08 
 
 P 2 O 5 
 
 .50 
 
 .26 
 
 .42 
 
 .50 
 
 .88 
 
 1.04 
 
 Fe 
 
 2.18 
 
 53. 33 
 
 46. 60 
 
 49. 81 
 
 54. 76 
 
 57.50 
 
 Mn 
 
 41. 59 
 
 
 
 
 
 
 P 
 
 .22 
 
 .11 
 
 .18 
 
 .22 
 
 .38 
 
 .45 
 
 S 
 
 .12 
 
 . 06 
 
 .03 
 
 .14 
 
 
 .02 
 
 
 
 
 
 Two manganese ores. Cripple Creek, eight miles from Wytheville, 
 Yirginia. Analyses by C. Catlett. 
 
 
 1. 
 
 } 
 
 2 . 
 
 SiO a 
 
 47. 30 
 
 27.86 
 
 Fe 
 
 2. 72 
 
 3. 61 
 
 Mn 
 
 24. 85 
 
 32. 55 
 
 P 
 
 .05 
 
 .097 
 
 S 
 
 trace 
 
 .030 
 
 Iron ore from Shanghai, West Yirginia. Analyzed by C. Catlett. 
 
 Si0 2 
 Fe . 
 Mu . 
 
 45.24 
 26 . 02 
 .43 
 
CATLETT.! 
 
 MISCELLANEOUS ANALYSES. 
 
 53 
 
 Two iron ores from Kentucky ; analyzed by J. E. Whitfield. A, 
 Cloverport Road, two miles north of Fordsville, Ohio County. B, north 
 slope of Pine Mountain, three miles east of Pineville, Bell County. 
 
 
 A. 
 
 B. 
 
 Si0 2 .............. 
 
 35. 67 
 
 17. 28 
 
 Ti0 2 
 
 trace 
 
 trace 
 
 Cl 
 
 trace 
 
 
 so 3 
 
 .42 
 
 .40 
 
 p 2 0 6 
 
 1.42 
 
 trace 
 
 ai 2 o 3 
 
 6. 15 
 
 .35 
 
 F © 2 0 3 
 
 42. 31 
 
 68. 24 
 
 FeO 
 
 .35 
 
 trace 
 
 MnO 
 
 .84 
 
 .95 
 
 CaO 
 
 1.90 
 
 .83 
 
 MgO 
 
 1. 07 
 
 .92 
 
 Ignition 
 
 9. 69 
 
 11. 60 
 
 
 99. 82 
 
 100. 57 
 
 Fe 
 
 29. 86 
 
 47.77 
 
 p 
 
 . 71 
 
 
 s 
 
 .16 
 
 .15 
 
 Iron ore. Douglass Mine, Clinton Horizon, one mile west of Big 
 Creek Gap, Campbell County, Tennessee. Analyzed by W. F. Hille- 
 brand. 
 
 Si0 2 
 
 Fe.. 
 
 Mn. 
 
 10. 51 
 54. 29 
 .20 
 
 P 355 
 
 S 043 
 
 Two iron ores ; analyzed by C. Catlett. A, from Edgefield County, 
 South Carolina. B, north part of Howard County, Arkansas. 
 
 
 A. 
 
 B. 
 
 Si0 2 ............ 
 
 9. 40 
 
 28.10 
 
 Fe 
 
 52. 40 
 
 29. 57 
 
 Mn 
 
 trace 
 
 2. 19 
 
 P 
 
 .664 
 
 .483 
 
 S 
 
 .08 
 
 .04 
 
54 
 
 WASHINGTON LABORATORY. 
 
 [RULL. 64. 
 
 10. COAL AND COKE. 
 
 Three coals. Raccoon Fork of Cabin Creek, Kanawha County, West 
 Virginia. Analyzed by E. L. Howard. 
 
 
 1 . 
 
 2. 
 
 3. 
 
 Moisture 
 
 1. 93 
 
 2. 15 
 
 1.67 
 
 Volatile matter . . . 
 
 37. 09 
 
 23. 95 
 
 41. 36 
 
 Fixed carbon 
 
 57. 90 
 
 61. 85 
 
 53. 22 
 
 Ash 
 
 3. 08 
 
 12. 05 
 
 3. 75 
 
 
 100.00 
 
 100. 00 
 
 100. 00 
 
 Sulphur 
 
 .62 
 
 .46 
 
 .80 
 
 Ash 
 
 dirty white 
 
 light gray 
 
 reddish 
 
 Coal and coke. Davis Mine No. 1, near North Fork of Blackwater, 
 Tucker County, West Virginia. Analyzed by Charles Catlett. 
 
 
 Coal. 
 
 Coke. 
 
 Moisture 
 
 .80 
 
 .18 
 
 Volatile., matter . . . 
 
 26. 84 
 
 1.49 
 
 Fixed carbon 
 
 67. 18 
 
 90. 60 
 
 Ash 
 
 5.18 
 
 7. 73 
 
 
 100. 00 
 
 100. 00 
 
 Sulphur 
 
 1.68 
 
 .771 
 
 Ash 
 
 very light red 
 
 light red 
 
 Five coals. Campbell County, Tennessee ; A, B, C analyzed by W. F. 
 Hillebrand; D, E by Charles Catlett. A, Douglass Bank, Middle Fork 
 of Big Creek, one and one half miles from Gap, lower coal-measures. 
 B, Walnut Mountain, head of Hickory Creek, Clear Fork of Cumber- 
 land River, 2,850 feet above sea-level, upper coal-measures. C, Middle 
 Fork of Big Creek, lower coal-measures. D, East Fork of Big Creek. 
 E, Middle Fork of Big Creek, three miles from Big Creek Gap. 
 
 
 A. 
 
 B. 
 
 C. 
 
 D. 
 
 E. 
 
 Moisture 
 
 1.49 
 
 2. 95 
 
 1.11 
 
 1.70 
 
 7. 60 
 
 Volatile matter... 
 
 39. 00 
 
 38. 51 
 
 35. 59 
 
 39.41 
 
 34. 89 
 
 Fixed carbon 
 
 53. 30 
 
 55.42 
 
 23. 99 
 
 55. 36 
 
 53. 14 
 
 Ash 
 
 6. 21 
 
 3. 12 
 
 39.31 
 
 3. 53 
 
 4. 37 
 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 S 
 
 1. 53 
 
 .87 
 
 2. 78 
 
 1. 07 
 
 .64 
 
 P 
 
 .041 
 
 
 
 
 
 
 
 
 
 
 
 A rough test on C showed that one ton of coal should yield 40,000 
 cubic feet of gas. 
 
BAKINS.] MISCELLANEOUS ANALYSES. 55 
 
 Also two cokes, analyzed by C. Catlett. F, Walnut Mountain, Hickory 
 Creek. G, from Sharp coal, Left Fork of Big Creek. 
 
 
 F. 
 
 G. 
 
 Moisture 
 
 .20 
 
 .50 
 
 Volatile matter... 
 
 2.01 
 
 1. 95 
 
 Fixed carbon 
 
 85. 56 
 
 91.71 
 
 Asb 
 
 12. 23 
 
 5.84 
 
 
 100. 00 
 
 100.00 
 
 S 
 
 .886 
 
 .705 
 
 P 
 
 .040 
 
 undet. 
 
 Thirty-two coals from Gunnison County, Colorado. Collected by G. H. 
 Eldridge, and analyzed by L. G. Eakins. 
 
 From Anthracite Creek Mines. 
 
 Moisture 3. 95 
 
 Volatile matter 4. 65 ' 
 
 Fixed carbon 82. 34 
 
 Ash 9.06 
 
 100. 00 
 
 .63 
 .07 
 
 Specific gravity 1.644 — 24.4° 
 
 Ash, light red $ no coke. 
 
 From Green Mountain, Denver Beds. 
 
 Moisture 8.91 
 
 Volatile matter 46.16 
 
 Fixed carbon 44.46 
 
 Ash 47 
 
 100. 00 
 
 .47 
 
 1. 381—22. 5° 
 
 S 
 
 Specific gravity 
 
 Ash, light red ; coke moderately coherent. 
 
 S 
 
 P. in ash 
 
56 
 
 WASHINGTON LABORATORY. 
 
 [BUHL. 64. 
 
 From Ohio Creek Mines, Nos. 1 to 11. 
 
 
 1. 
 
 2. 
 
 3. 
 
 4. 
 
 5. 
 
 Moisture 
 
 7.39 
 
 8. 46 
 
 8. 26 
 
 1.61 
 
 1. 34 
 
 Volatile matter 
 
 39.43 
 
 39. 01 
 
 39. 96 
 
 13. 05 
 
 30. 25 
 
 Fixed carbon 
 
 47.83 
 
 46. 68 
 
 46. 36 
 
 80. 29 
 
 62. 38 
 
 Ash 
 
 5. 35 
 
 5. 85 
 
 5.42 
 
 5. 05 
 
 6.03 
 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 s 
 
 1.47 
 
 .76 
 
 .68 
 
 .59 
 
 .44 
 
 P. in ash 
 
 
 
 .06 
 
 
 .07 
 
 Specific gravity 
 
 1.328, 23° 
 
 1.334, 21.6° 
 
 1.331, 25° 
 
 1.407, 23° 
 
 1.325, 22o 
 
 Ash 
 
 reddish gray .... 
 
 light rod 
 
 light red 
 
 red 
 
 red 
 
 Coke 
 
 fairly coherent 
 
 cokes slightly 
 
 cokes slightly. 
 
 none 
 
 firm, solid. 
 
 
 6. 
 
 7. 
 
 8. 
 
 9. 
 
 10. 
 
 11. 
 
 Moisture 
 
 6. 28 
 
 6. 37 
 
 6. 39 
 
 1.07 
 
 1. 23 
 
 .81 
 
 Volatile matter. 
 
 40. 92 
 
 38. 06 
 
 39. 26 
 
 26. 22 
 
 26. 65 
 
 9. 96 
 
 Fixed carbon . . . 
 
 46. 35 
 
 49. 75 
 
 48.41 
 
 68. 36 
 
 68. 27 
 
 82. 33 
 
 Ash 
 
 6. 45 
 
 5. 82 
 
 5. 94 
 
 4. 35 
 
 3. 85 
 
 6. 90 
 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 S 
 
 .47 
 
 .46 
 
 .46 
 
 .60 
 
 .61 
 
 1. 06 
 
 P. in ash 
 
 
 
 .03 
 
 .05 
 
 
 
 Specific gravity. 
 
 1.324, 210 
 
 „ 1.345, 21.6° 
 
 1.337, 23° 
 
 1.319, 22° 
 
 1.317, 22° 
 
 1.426, 23.8° 
 
 Ash 
 
 reddish yellow 
 
 reddish yellow . . 
 
 red 
 
 red 
 
 red 
 
 pinkish gray. 
 
 Coke 
 
 fair 
 
 slightly coherent 
 
 fair 
 
 fair 
 
 fair 
 
 none 
 
 
 
 
 
 
 
 From Slate Creek Mines, Nos. 12 to 21. 
 
 
 12. 
 
 13. 
 
 14 
 
 15. 
 
 16. 
 
 Moisture 
 
 1. 29 
 
 1.36 
 
 1.86 
 
 1. 35 
 
 1.30 
 
 Volatile matter 
 
 7. 92 
 
 7. 53 
 
 6. 68 
 
 6. 59 
 
 7. 55 
 
 Fixed carbon 
 
 85. 71 
 
 85.49 
 
 86. 25 
 
 72. 34 
 
 80. 44 
 
 Ash 
 
 5. 08 
 
 5.62 
 
 5.21 
 
 19.72 
 
 10.71 
 
 
 100. 00 
 
 100.00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 S 
 
 .67 
 
 .54 
 
 .69 
 
 .66 
 
 .58 
 
 P. in ash 
 
 
 .4)5 
 
 . 03 
 
 
 .32 
 
 Specific gravity 
 
 1.428, 23.4° 
 
 1.440, 21.8° 
 
 1.465, 26.40 
 
 1.481, 22.2° 
 
 1.502, 22.8° 
 
 Ash.. 
 
 red 
 
 red 
 
 red _ 
 
 prrav ...... 
 
 light red . . 
 
 Coke 
 
 non© ...... 
 
 non© 
 
 non© 
 
 non© 
 
 non© 
 
 
 
 
 
 
 
 
 17. 
 
 18. 
 
 19. 
 
 20. 
 
 21. 
 
 Moisture 
 
 1.58 
 
 1. 22 
 
 1.27 
 
 .92 
 
 .81 
 
 Volatile matter 
 
 6. 70 
 
 8.46 
 
 7. 99 
 
 14. 19 
 
 13.40 
 
 Fixed carbon 
 
 87. 46 
 
 84. 20 
 
 87.24 
 
 81. 29 
 
 81.26 
 
 Ash 
 
 4.26 
 
 6. 12 
 
 3. 50 
 
 3. 60 
 
 4.53 
 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100.00 
 
 100. 00 
 
 S 
 
 .58 
 
 . 76 
 
 .^2 
 
 • 52 
 
 .51 
 
 P. in ash 
 
 
 
 
 non© 
 
 
 Specific gravity. .. 
 
 1.455, 22.8° 
 
 1.409, 22° 
 
 1.409, 23.3° 
 
 1.359, 20.4° 
 
 1.371, 20 8° 
 
 A ah - 
 
 red 
 
 red 
 
 red 
 
 light red 
 
 red 
 
 Coke.... 
 
 non© 
 
 none 
 
 non© 
 
 cokes slightly. 
 
 cokes slightly. 
 
 
 
 
 
CEATAED.] 
 
 MISCELLANEOUS ANALYSES, 
 
 57 
 
 From Crested Butte Mines, Nos. 22 to 30. 
 
 
 22. 
 
 23. 
 
 24. 
 
 25. 
 
 Moisture 
 
 
 
 1. 36 
 
 1.47 
 
 1. 94 
 
 2. 36 
 
 Volatile matter. . 
 
 
 
 37. 12 
 
 38. 09 
 
 41.07 
 
 40. 82 
 
 Fixed carbon 
 
 
 
 57.73 
 
 56. 68 
 
 51.48 
 
 50.49 
 
 Ash 
 
 
 
 3. 79 
 
 3. 76 
 
 5. 51 
 
 6. 33 
 
 
 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 S 
 
 
 
 
 49 
 
 
 ,47 
 
 .63 
 
 1.04 
 
 
 
 
 
 
 
 07 
 
 trace 
 
 
 Specific gravity 
 
 
 
 1.288, 22.6° 
 
 1.276, 21° 
 
 1.311, 21.1° 
 
 1.332, 22° 
 
 A ah 
 
 
 
 licrht red 
 
 licrht _ . 
 
 red 
 
 red 
 
 flotft 
 
 trend 
 
 
 creed _ 
 
 
 good 
 
 good 
 
 
 
 
 
 
 
 26. 
 
 27. 
 
 28. 
 
 29. 
 
 30. 
 
 Moisture 
 
 1. 88 
 
 
 2. 09 
 
 
 1.76 
 
 
 3. 95 
 
 4. 83 
 
 Volatile matter. 
 
 39. 51 
 
 
 41.74 
 
 
 42. 00 
 
 
 37. 17 
 
 37. 86 
 
 Fixed carbon ... 
 
 54. 42 
 
 
 52.07 
 
 
 51. 97 
 
 
 52. 34 
 
 51. 65 
 
 Ash 
 
 4. 19 
 
 
 4. 10 
 
 
 4. 27 
 
 
 6. 54 
 
 5. 66 
 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 100. 00 
 
 s 
 
 .63 
 
 
 .65 
 
 
 .75 
 
 
 .42 
 
 .68 
 
 P. in ash 
 
 
 trace 
 
 
 
 
 
 
 Specific gravity. 
 
 1.288, 24.8° 
 
 1.289, 26.6° 
 
 1.286, 20° 
 
 
 1.328, 22.4° 
 
 1.349, 21.20 
 
 A ah 
 
 red 
 
 red 
 
 light red . . 
 
 red 
 
 red 
 
 Celt a. 
 
 good, solid 
 
 (rend 
 
 trend 
 
 hn/rrl cnnmuct. 
 
 fair 
 
 
 
 
 
 
 
 
 
 11. ANALYSES OF WATERS. 
 
 Analyzed by T. M. Chatard. A, from the Murray Well, one mile 
 north of Frankfort, Kentucky. Slight odor of H 2 S. Specific gravity, 
 .99984, 22°. 
 
 
 Found, 
 grammes 
 per liter. 
 
 Per cent, 
 of total 
 contents. 
 
 
 Combina- 
 
 tion. 
 
 Rif) 2 
 
 .0096 
 
 .61 
 
 C0 2 
 
 .0172 
 
 Fe 
 
 .0014 
 
 .08 
 
 nh 3 
 
 .0015 
 
 Ca 
 
 .0213 
 
 1.35 
 
 KC1 
 
 .0396 
 
 Sr? 
 
 .0122 
 
 . 71 
 
 NaCl 
 
 .8287 
 
 Mg 
 
 .0189 
 
 1.20 
 
 Na 2 S0 4 . .. 
 
 .2770 
 
 K 
 
 .0207 
 
 1.31 
 
 FaH 2 C 2 O c 
 
 . 0045 
 
 Na 
 
 .4604 
 
 29. 35 
 
 CaH 2 n 2 O c . . 
 
 . 0862 
 
 Li 
 
 trace 
 
 
 SrTTjjftjOg? 
 
 .0269 
 
 SO* 
 
 .1873 
 
 11.93 
 
 MvTToCoO^ 
 
 .1150 
 
 
 
 
 
 
 
 Cl 
 
 .5218 
 
 33. 23 
 
 NaHCOs 
 
 .1639 
 
 COJ 
 
 .2929 
 
 18. 74 
 
 Si0 2 ... 
 
 .0096 
 
 C0 2 , free 
 
 .0172 
 
 1.09 
 
 
 NH S 
 
 .0015 
 
 .09 
 
 
 
 H, in bicarbonates 
 
 .0049 
 
 .31 
 
 
 
 
 1. 5701 
 
 100. 00 
 
 
 1. 5701 
 
 The strontium is doubtful, and may be only a strong trace. 
 
58 
 
 WASHINGTON LABORATORY, 
 
 [BULL. 64; 
 
 B, spring water from Mountain City, Tennessee. Statement like the 
 preceding. 
 
 
 Found. 
 
 Per cent, 
 of total. 
 
 
 Combina- 
 
 tion. 
 
 
 . 0219 
 
 21. 26 
 
 Si0 2 
 
 . 0219 
 
 Fe 
 
 .0008 
 
 .78 
 
 FeH 2 C206 
 
 .0026 
 
 A1 
 
 trace 
 
 
 CaH 2 C 2 0 6 
 
 .0448 
 
 Ca 
 
 .0116 
 
 11. 26 
 
 MjrHoC„0, 
 
 .0110 
 
 Mg 
 
 .0018 
 
 1. 75 
 
 b * ^ •*••■**• 
 
 CaS0 4 
 
 .0018 
 
 Na 
 
 .0046 
 
 4. 47 
 
 Na 2 S0 4 
 
 .0142 
 
 K 
 
 .0032 
 
 3. 11 
 
 k 2 so 4 
 
 .0042 
 
 Cl 
 
 .0012 
 
 1. 16 
 
 KC1 
 
 .0025 
 
 so 4 
 
 .0132 
 
 12. 81 
 
 
 
 COg 
 
 .0440 
 
 42. 72 
 
 
 
 H, bicarbonates .. 
 
 .0007 
 
 .68 
 
 
 
 
 .1030 
 
 100. 00 
 
 
 .1030 
 
 C, the Grace Spring, seven miles north of Mountain City, Tennessee, 
 on the road to Abingdon, Virginia, near Laurel Bloomery post-office. 
 Specific gravity, 1.00038, 18.5°. 
 
 
 Found. 
 
 Per cent, 
 of total. 
 
 
 Combina- 
 
 tion. 
 
 SiOj 
 
 .0125 
 
 1. 09 
 
 Si0 2 
 
 .0125 
 
 Fe 
 
 trace 
 
 
 KC1 
 
 .0023 
 
 Ca 
 
 .2334 
 
 20. 31 
 
 KoSOjj 
 
 .0075 
 
 Mg 
 
 .0580 
 
 5. 05 
 
 Na 2 S0 4 
 
 .0145 
 
 K 
 
 . 0046 
 
 .40 
 
 MgS0 4 
 
 . 2900 
 
 Na 
 
 .0047 
 
 .41 
 
 CaS0 4 
 
 .6429 
 
 Cl 
 
 .0011 
 
 .09 
 
 CaTLjCoOg 
 
 . 1794 
 
 so 4 
 
 .6997 
 
 60. 89 
 
 
 
 COg 
 
 .1329 
 
 11.57 
 
 
 
 H, bicarbonates. . . 
 
 .0022 
 
 .19 
 
 
 
 
 1. 1491 
 
 100. 00 
 
 
 1. 1491 
 
chatard.] MISCELLANEOUS ANALYSES. 59 
 
 D, drinking water, Savannah, Georgia. Stated in grammes per liter. 
 
 
 Found. 
 
 
 Combina- 
 
 tion. 
 
 Suspended matter (organic) . . . 
 
 .0020 
 
 Suspended matter 
 
 .0025 
 
 Suspended matter (inorganic). 
 
 .0005 
 
 Si0 2 
 
 .0624 
 
 Si0 2 
 
 .0624 
 
 -A.I 0 O 5 . FcoOq 
 
 .0006 
 
 AlA, Fe s O* 
 
 .0006 
 
 NaCl 
 
 . 0097 
 
 Ca 
 
 .0279 
 
 Na 2 S0 4 
 
 .0120 
 
 Mg 
 
 . 0085 
 
 CaH 2 C 2 0 6 
 
 .1129 
 
 
 
 
 
 Na 
 
 .0075 
 
 MgTT 2 CnO c . . 
 
 .0517 
 
 Cl 
 
 .0061 
 
 
 S0 4 
 
 .0081 
 
 
 
 C0 3 
 
 .1262 
 
 
 
 NH 3 , free 
 
 trace 
 
 
 
 NH 3 , albuminoid 
 
 none 
 
 
 
 H, bicarbonates 
 
 .0020 
 
 
 
 
 .2518 
 
 
 .2518 
 
 E, two artesian well waters from St. Augustine, Florida, (a) six- 
 incli well. 
 
 
 Found. 
 
 Per cent, 
 of total. 
 
 • 
 
 Combina- 
 
 tion. 
 
 Suspended matter. 
 
 .0037 
 
 .24 
 
 Suspended matter. 
 
 .0037 
 
 Si0 2 
 
 .0224 
 
 1.43 
 
 Si0 2 
 
 .0224 
 
 A 1 2 O 3 
 
 .0005 
 
 .03 
 
 A1 2 0 3 
 
 .0005 
 
 Ca 
 
 .1276 
 
 8.16 
 
 NaCl 
 
 .6979 
 
 Mg 
 
 .0726 
 
 4. 64 
 
 KC1 
 
 .0281 
 
 Sr 
 
 .0081 
 
 .52 
 
 MgCl 2 
 
 .1470 
 
 Na 
 
 .2743 
 
 17. 54 
 
 SrSO t 
 
 .0170 
 
 K 
 
 .0147 
 
 .94 
 
 CaSO, 
 
 .4338 
 
 Cl 
 
 .5469 
 
 34. 97 
 
 MgS0 4 
 
 .0127 
 
 S0 4 
 
 .3253 
 
 20.81 
 
 MgHoC 2 0 6 
 
 .2007 
 
 C0 3 
 
 .1650 
 
 10. 55 
 
 OaTTjfJjOj - 
 
 none. 
 
 H, bicarbonates... 
 
 .0027 
 
 .17 
 
 
 
 1. 5638 
 
 100. 00 
 
 
 1. 5638 
 
60 WASHINGTON LABORATORY. [bull. 64. 
 
 (b) twelve-inch well. 
 
 
 Found. 
 
 Per cent, 
 of total. 
 
 
 Combina- 
 
 tion. 
 
 Suspended matter. 
 
 .0016 
 
 .05 
 
 Suspended matter . 
 
 .-0016 
 
 Si0 2 
 
 .0280 
 
 .88 
 
 SiO« 
 
 . 0280 
 
 AljOj 
 
 .0012 
 
 ' .04 
 
 A1 2 0 3 
 
 .0012 
 
 Ca 
 
 .1755 
 
 5. 50 
 
 UaCl 
 
 1. 9577 
 
 Mg 
 
 .1160 
 
 3. 64 
 
 KC1 
 
 .0475 
 
 Sr 
 
 . 0089 
 
 .28 
 
 MeClo 
 
 . 3534 
 
 Na 
 
 .7695 
 
 24.12 
 
 - 1JA te vyx 2 
 
 SrS0 4 ... 
 
 .0186 
 
 K 
 
 .0248 
 
 .77 
 
 CaS0 4 
 
 . 4709 
 
 Cl 
 
 1. 4750 
 
 46. 22 
 
 M<rS0 4 
 
 none. 
 
 S0 4 
 
 .3421 
 
 10. 73 
 
 Mp'TToCi.O* 
 
 .1621 
 
 C0 3 
 
 .2442 
 
 7. 64 
 
 " A h- LX z v i v/ 6 
 
 CaH 2 C 2 O c 
 
 .1499 
 
 H, bicarbonate s . . . 
 
 .0041 
 
 .13 
 
 
 
 
 3. 1909 
 
 100. 00 
 
 - 
 
 3. 1909 
 
 F, from well four miles northwest of Clinton, Hinds County, Missis- 
 sippi. No carbonates present. 
 
 
 Found. 
 
 Percent, 
 of total. 
 
 
 Combina- 
 
 tion. 
 
 • 
 
 Suspended matter. 
 
 .0028 
 
 .18 
 
 Suspended matter. 
 
 .0028 
 
 Sif) 2 
 
 .0750 
 
 4. 82 
 
 Si0 2 
 
 .0750- 
 
 Al 2 f) 3 
 
 .0077 
 
 .49 
 
 A1 2 0 3 
 
 .0077 
 
 Fe^Oj 
 
 trace. 
 
 
 A1,(S0 4 )* 
 
 .0504 
 
 A1 in sulphate 
 
 .0081 
 
 .52 
 
 MnSC>4 
 
 .0028 
 
 Mn 
 
 . 0010 
 
 .06 | 
 
 CaS0 4 
 
 .6732 
 
 Ca 
 
 .1980 
 
 12. 72 
 
 MgS0 4 
 
 .3695 
 
 Mer 
 
 .0739 
 
 4. 78 
 
 ^Ta.iSOj 
 
 .2519 
 
 "•o - -- -- -- - 
 
 Na 
 
 . 1234 
 
 7. 92 
 
 NaCl 
 
 . 1063 
 
 K 
 
 .0088 
 
 .56 
 
 KC1 
 
 .0167 
 
 S0 4 
 
 .9852 
 
 63.30 
 
 
 
 Cl 
 
 .0724 
 
 4. 65 
 
 
 
 
 1. 5563 
 
 100.00 
 
 
 1. 5563 
 
 O 
 
Title for subject entry. Author title. Series title. 
 
 LIBRARY CATALOGUE SLIPS. 
 
 United States. Department of the interior. ( U. S. geological survey.) 
 Department of the interior | — | Bulletin | of the | United 
 States | geological survey | no. 65 | [Seal of the department] | 
 Washington | government printing office | 1891 
 
 Second title: United States geological survey | J. W. Powell, 
 director | — | Stratigraphy | of the | bituminous coal field | of | 
 Pennsylvania, Ohio, and West Virginia | by | Israel C. White j . 
 [Vignette] | 
 
 Washington | government printing office | 1891 
 
 8°. 212 pp. 11 pL 
 
 White (Israel C.). 
 
 United States geological survey | J. W. Powell, director | — | 
 Stratigraphy | of the | bituminous coal field | of | Pennsylvania, 
 Ohio, and West Virginia | by | Israel C. White | [Vignette] 
 Washington | government printing office | 1891 
 
 8°. 212 pp. 11 pi. 
 
 [United States. Department oj the interior. ( U . . S . geological survey.) 
 Bulletin 65.] 
 
 United States geological survey | J. W. Powell, director | — | 
 Stratigraphy | of the | bituminous coal field | of | Pennsylvania, 
 Ohio, and West Virginia | by | Israel C. White | [Vignette] 
 Washington | government printing office | 1891 
 
 8°. 212 pp. 11 pi. 
 
 [United States. Department qf the interior. (U. S. geological survey.) 
 Bulletin 65.] 
 
ADYKETISEMENT 
 
 [Bulletin No. 65.] 
 
 The publications of the United States Geological Survey are issued in accordance with the statute 
 approved March 3, 1879, which declares that — 
 
 “ The publications of the Geological Survey shall consist of the annual report of operations, geological 
 and economio maps illustrating the resources and classification of the lands and reports upon general 
 and economic geology and paleontology. The annual report of operations of the Geological Survey 
 shall accompany the annual report of the Secretary of the Interior. All special memoirs and reports 
 of said Survey shall be issued in uniform quarto series if deemed necessary by the Director, but other- 
 wise in ordinary octavos. Three thousand copies of each shall be published for scientific exchanges 
 and for sale at the price of publication ; and all literary and cartographic materials received in exchange 
 shall be the property of the United States and form a part of the library of the organization • and the 
 money resulting from the sale of such publications shall be covered into the Treasury of the United 
 States.” 
 
 On July 7, 1882, the following joint resolution, referring to all Government publications, was passed 
 by Congress: 
 
 “ That whenever any document or report shall be ordered printed by Congress, there shall be printed, 
 in addition to the number in each case stated, the ‘usual number’ (1,900) of copies for binding and 
 distribution among those entitled to receive them.” 
 
 Except in those cases in which an extra number of any publication has been supplied to the Survey 
 by special resolution of Congress or has been ordered by the Secretary of the Interior, this office has 
 no copies for gratuitous distribution. 
 
 ANNUAL REPORTS. 
 
 L First Annual Report of the United States Geological Survey, by Clarence King. 1880. 8°. 79 pp. 
 1 map. — A preliminary report describing plan of organization and publications. 
 
 II. Second Annual Report of the United States Geological Survey, 1880-81, by J. W. Powell. 1882. 
 8°. lv, 588 pp. 62 pi. 1 map. 
 
 III. Third Annual Report of the United States Geological Survey, 1881-’82, by J. W. Powell. 1883. 
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 TV. Fourth Annual report of the United States Geological Survey, 1882-83, by J. W. Powell. 1884. 
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 Y. Fifth Annual Report of the United States Geological Survey, l883-’84, by J. W. Powell. 1885* 
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 YI. Sixth Annual Report of the United States Geological Survey, 1884-’85, by J. W. Powell. 1885. 
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 VXL Seventh Annual Report of the United States Geological Survey, 1885-’86, by J. W. Powell. 1888. 
 8°. xx, 656 pp. 71 pi. and maps. 
 
 Tin. Eighth Annual Report of the United States Geological Survey, 1886-’87, by J. W. Powell. 1889. 
 8° 2v. xix, 474, xii pp. 53 pi. and maps ; 1 p. 1. 475-1063 pp. 54-76 pi. and maps. 
 
 IX. Ninth Annual Report of the United States Geological Survey, 1887- ’88, by J. W. Powell. 1889. 
 8°. xiii, 717 pp. 88 pi. and maps. 
 
 X. Tenth Annual Report of the United States Geological Survey, 1888-’89, by J. W. Powell. 1890. 
 8°. 2 v. xv, 774 pp. 98 pi. and maps ; viii, 123 pp. 
 
 The Eleventh Annual Report is in press. 
 
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 Washington, D. C., December, 1890 
 
DEPARTMENT OF THE INTERIOR 
 
 BULLETIN 
 
 OF THE 
 
 UNITED STATES 
 
 GEOLOGICAL SURVEY 
 
 INo. 
 
 6 5 
 
 WASHINGTON 
 
 GOVERNMENT PRINTING OFFICE 
 1891 
 
UNITED STATES GEOLOGICAL SURVEY 
 
 J. W. POWELL, DIRECTOR 
 
 STRATIGRAPHY 
 
 OF THE 
 
 / 
 
 BITUMINOUS COAL FIELD 
 
 PENNSYLVANIA, OHIO AND WEST VIRGINIA 
 
 BY 
 
 ISRAEL C. WHITE 
 
 WASHINGTON 
 
 GOVERNMENT PRINTING OFFICE 
 1891 
 

 ' 
 
 . ... ' ■ 
 
 V 
 
 - 
 
 
 
 
 
 
 
 
 ■ 
 
 i; . ■■■ ■' ' 7 
 
 
 
 . 
 
 
 
 
 / 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
CONTENTS 
 
 ■ 
 
 Page. 
 
 Letter of transmittal 15 
 
 Chap. I. — Area, structure, and classification of the bituminous coal rocks 17 
 
 Chap. II. — The Permo-Carboniferous or Dunkard Creek Measures 20 
 
 Thickness, character, and extent 20 
 
 Section on Dunkard Creek, Greene Co., Pa 22 
 
 Section on Colvin’s Run, Greene Co., Pa 23 
 
 Section in Aleppo Township, Greene Co., Pa 24 
 
 Section at Board Tree Tunnel, Marshall Co., W. Ya 25 
 
 Section at Bellton, Marshall Co., W. Ya 26 
 
 Section at New Martinsville, Wetzel Co., W. Ya 27 
 
 Section at Baresville, Monroe Co., Ohio 28 
 
 Section in Liberty Township, Washington Co., Ohio 29 
 
 Section at Washington, Washington Co., Pa 29 
 
 Section near Taylorstown, Washington Co., Pa 30 
 
 Characteristic horizons 30 
 
 The Windy Gap Limestone 30 
 
 The Windy Gap Coal 31 
 
 The Gilmore Sandstone 31‘ 
 
 The Nineveh Sandstone 32 
 
 The Bellton Coal Group 32 
 
 The Nineveh Coal 32 
 
 The Nineveh Limestone 32 
 
 The Hostetter Coal 33 
 
 The Fish Creek Sandstone 33 
 
 The Dunkard Coal 33 
 
 The Jollytown Limestone 34 
 
 The Jollytown Coal 34 
 
 The Upper Washington Limestone t 35 
 
 The Middle Washington Limestone 35 
 
 The Washington “A” Coal 35 
 
 The Marietta Sandstones 35 
 
 The Blacksville Limestone 36 
 
 The Lower Washington Limestone 36 
 
 The Washington Coal 37 
 
 Section at Farmington, Marion Co., W. Va 37 
 
 Section on Willey Fork, Wetzel Co., W. Va 38 
 
 Section near Brown’s Mill, Monongalia Co., W. Va 38 
 
 The Washington Sandstone 1 38 
 
 The Little Washington Coal 39 
 
 The Waynesburg “ B” Coal 39 
 
 The Colvin’s Run Limestone 39 
 
 The Waynesburg “A” Coal 39 
 
 The Mount Morris Limestone 39 
 
 The Waynesburg Sandstone 40 
 
 The Cassville Plant Shale 41 
 
 Age of the Dunkard Creek Beds 41 
 
 5 
 
6 
 
 CONTENTS, 
 
 Page. 
 
 Chap. III. The Upper Coal Measures, or Monongaliela River Series 43 
 
 Thickness, character, and, extent 43 
 
 Section in Fayette and Westmoreland Cos., Pa 44 
 
 Section at Brownsville, Fayette Co., Pa 44 
 
 Section at West Brownsville, Washington Co., Pa 45 
 
 Section at Rice’s Landing, Greene Co., Pa 45 
 
 Section on Robinson’s Run, Monongalia Co., W. Va 46 
 
 Section on Scott’s Run, Monongalia Co., W. Va ! 47 
 
 Section on Buffalo Creek, Marion Co., W. Va 48 
 
 Section at Clarksburg, Harrison Co., W. Va 48 
 
 Section on Chapline Hill, Wheeling, W. Va 49 
 
 Section near Bellaire, Belmont Co., Ohio 50 
 
 Section at Moundsville, Marshall Co , W. Ya 51 
 
 Section on Pipe Creek, Belmont Co., Ohio 51 
 
 Section in Washington Co., Ohio 52 
 
 Section at Burning Springs, Wirt Co., W. Ya 52 
 
 Section on Leading Creek, Gilmer Co., W. Ya 53 
 
 Section at Antiquity, Meigs Co., Ohio 53 
 
 Section at Hartford City, Mason Co., W. Ya 53 
 
 Section at Arbuckle, Mason Co., W. Va 54 
 
 Section at mouth of Big Hurricane Creek, Putnam Co., W. Ya . ... 55 
 
 Section opposite V^infield, Putnam Co., W. Ya 5 o 
 
 Section near Raymond City, Putnam Co., W. Ya 56 
 
 Section in vicinity of Westernport, Allegany Co., Md 56 
 
 Characteristic horizons 57 
 
 The Waynesburg Coal 57 
 
 Iron Ore 57 
 
 The Browntown Sandstone 58 
 
 The Little Waynesburg Coal 58 
 
 The Waynesburg Limestone 58 
 
 The Uniontown Sandstone 58 
 
 The Uniontown Coal 59 
 
 The Uniontown Limestone 59 
 
 The “ Great” Limestone 59 
 
 The Sewickley Sandstone 60 
 
 The Sewickley Coal 60 
 
 The Sewickley Limestone 61 
 
 The Redstone Coal 62 
 
 The Redstone Limestone 62 
 
 The Pittsburgh Saudstone 63 
 
 The Pittsburgh Coal 63 
 
 Section at Newburgh, Preston Co., W. Va 65 
 
 Section in Copeman’s Knob, Preston Co., W. Va 65 
 
 Section at Fairfax Knob, Tucker Co., W. Ya 65 
 
 Section at Huntington, Cabell Co., W. Ya 66 
 
 Section at Pomeroy, Ohio 66 
 
 Section on Shade Creek, Meigs and Athens Cos., Ohio 66 
 
 Section on Federal Creek, Athens and Morgan Cos., Ohio 67 
 
 Section at Berry’s mine, in Homer Township, Morgan Co., Ohio .. 67 
 
 Section in Washington Township, Belmont Co., Ohio • 67 
 
 Section at Heatherington’s mine, at Bellaire, Belmont Co., Ohio .. 68 
 
 Section in Warren Township, Jefferson Co., Ohio 68 
 
 Section in German Township, Harrison Co., Ohio 68 
 
 Section at Columbia mine, Westmoreland Co., Pa 68 
 
 Fossils of the Upper Coal Measures 69 
 
CONTENTS. 
 
 7 
 
 Page. 
 
 Chap. IV. The Barren Measures, or Elk River Series 70 
 
 Thickness, character, and extent 70 
 
 Section in Pittsburgh region 72 
 
 Section at Sewickley, Pa 73 
 
 Section on Dunbar Creek, Fayette Co., Pa 74 
 
 Section at Ligonier, Westmoreland Co., Pa 75 
 
 Section in vicinity of Berlin, Somerset Co., Pa 76 
 
 Section in Broad Top Basin, Bedford Co., Pa 76 
 
 Section opposite Steubenville, Ohio 77 
 
 Section under Washington, Pa 77 
 
 Section near Cannonsburg, Washington Co., Pa 78 
 
 Section at Morgantown, W. Ya 79 
 
 Section near Little Falls, Monongalia Co., W. Va 80 
 
 Section at Newburg, Preston Co., W. Ya 81 
 
 Section at Fairfax Knob, Tucker Co., W. Va 82 
 
 Section in Guernsey Co., Ohio 83 
 
 Section at Burning Springs, Wirt Co., W. Ya 83 
 
 Section in vicinity of Huntington, W. Va 84 
 
 Section near Charleston, W. Ya 85 
 
 Characteristic horizons 86 
 
 The Pittsburgh Coal Ores 86 
 
 The Little Pittsburgh Coal 86 
 
 The Pittsburgh Limestones 87 
 
 The Connellsville Sandstone 87 
 
 The Little Clarksburg Coal 88 
 
 The Clarksburg Limestone 88 
 
 The Morgantown Sandstone 88 
 
 The Elk Lick Coal 89 
 
 Thb Elk Lick Limestone 90 
 
 The Crinoidal, Green Fossiliferous, or Ames Limestone 90 
 
 The Crinoidal Coal 91 
 
 The Red Shale Beds 92 
 
 The Bakersto wn Coal 92 
 
 The Cambridge Li mestoues 93 
 
 The Masontown Coal 94 
 
 The Irondale Limestone and Ore 95 
 
 The Mahoning Sandstone 95 
 
 The Mahoning Coal 96 
 
 The Mahoning Limestone . 96 
 
 The Upper and Middle Cannelton Coals 97 
 
 The Kanawha Black Flint 98 
 
 Chap. V. The Lower Coal Measures, or Alleghany River Series 99 
 
 Thickness, character, and extent 99 
 
 Section at Blossburg, Tioga Co., Pa 102 
 
 Section at Fall Brook, Tioga Co., Pa 103 
 
 Section at Karthaus, Clearfield Co., Pa 103 
 
 Section in Horton Towriship, Elk Co., Pa 104 
 
 Section at Brockwayville, Jefferson Co., Pa.. 104 
 
 Section in Clarion Co., Pa 105 
 
 Section at Miller’s Eddy, Clarion Co., Pa 105 
 
 Section at East Brady, Clarion Co., Pa 106 
 
 Section near New Bethlehem, Clarion Co., Pa 106 
 
 Section in Brady Township, Butler Co., Pa 107 
 
 Section at Ore Hill Furnace, Armstrong Co., Pa 107 
 
 Section at Centerville, Armstrong Co., Pa.„ 108 
 
8 
 
 CONTENTS, 
 
 Page. 
 
 Chap. V. The Lower Coal Measures, or Alleghany River Series— Continued. 
 
 Section at Putney ville, Armstrong Co., Pa 108 
 
 Section in vicinity of Kittanning, Pa 100 
 
 Section 5 miles below Kittanning, Pa 109 
 
 Section at Logansport, Armstrong Co., Pa 110 
 
 Section at Freeport, Armstrong Co., Pa Ill 
 
 Section near mouth of Beaver River 112 
 
 Section under Sewickley, Allegheny Co., Pa 112 
 
 Section under Washington, Pa 113 
 
 Section near Carpenter’s Station, Westmoreland Co., Pa 113 
 
 Section under Murraysvilie, Westmorelaud Co., Pa 114 
 
 Section on Beaver Run, Westmoreland Co., Pa 114 
 
 Section near Richmond, Indiana Co., Pa 115 
 
 Section near Lockport and Bolivar, Indiana Co., Pa 115 
 
 Section near Laughlinton, Westmoreland Co., Pa 116 
 
 Section on Cucumber Run, Stewart Township, Fayette Co., Pa 116 
 
 Section under Newburg, Preston Co., W. Ya 117 
 
 Section near Johnstown, Cambria Co., Pa 118 
 
 Section at Conemaugh, near Johnstown, Cambria Co., Pa 119 
 
 Section in Jackson Township, Cambria Co., Pa 119 
 
 Section on Ben’s Creek, Cambria Co., Pa 120 
 
 Section at Stoyestown, Somerset Co., Pa 121 
 
 Section at Pinkerton Point, Somerset Co., Pa 121 
 
 Section at Cresson, Cambria Co., Pa 122 
 
 Section at Bennington, Blair Co., Pa 122 
 
 Section at Clearfield, "Clearfield Co., Pa 123 
 
 Section near Morrisdale, Clearfield Co., Pa 123 
 
 Section at Sterling mines, near Houtzdale, Clearfield Co., Pa 124 
 
 Section on Shoup’s Run, Broad Top Basin, Huntingdon Co., Pa 125 
 
 Section in East Broad Top Basin, Huntingdon Co., Pa 125 
 
 Section in Broad Top Basin, Bedford Co., Pa 126 
 
 Section at Piedmont, Mineral Co., W. Ya 126 
 
 Section at Maple Swamp water tank, W. Ya. Central Railroad 127 
 
 Section near Thomas, Tucker Co., W. Ya 127 
 
 Section near Moatsville, Barbour Co., W. Va 128 
 
 Section at Yalley Falls, Taylor Co., W. Va 128 
 
 Section near Nuzum’s Mills, Marion Co., W. Va 129 
 
 Section under Clarksburg, Harrison Co., W. Ya 129 
 
 Section under Parkersburg, W. Va 130 
 
 Section under Wheeling, W. Va 130 
 
 Section at mouth of Little Beaver, on the Ohio-Penusylvauia line 130 
 
 Section near Sprucevale, Columbiana Co., Ohio 131 
 
 Section between New Lisbon and Leetonia, Ohio 132 
 
 Section at Zanesville, Muskingum Co., Ohio 132 
 
 Section in vicinity of Shawnee and McCuneville, Perry Co., Ohio 133 
 
 Section in Hocking Yalley, near Buchtel, Ohio 133 
 
 Section on Meeker’s Run, near Nelsonville, Athens Co., Ohio 134 
 
 Section in Panther Hill, Mt. Vernon Furnace, Scioto Co., Ohio 134 
 
 Section at Ironton, Lawrence Co., Ohio 135 
 
 Section in southern Ohio, above Ironton , 135 
 
 Section under Charleston, W. Ya 136 
 
 Section at mouth of Lick Run, 2 miles above Charleston, W. Va 137 
 
 Section at Dickinson Salt Works, Kanawha Co., W. Va 138 
 
 Section near Brownstown, 3 miles south from Malden, W. Ya 139 
 
 Section at mouth of Armstrong Creek, on the Big Kanawha River 140 
 
CONTENTS, 
 
 9 
 
 Page. 
 
 Chap. V. The Lower Coal Measures, or Alleghany River Series — Continued. 
 
 Section at Guyandotte Mountain, Raleigh Co., W. Va 142 
 
 Section near Oceana, Wyoming Co., W. Va 143 
 
 Section at mouth of Blaine Creek, Lawrence Co., Ky 144 
 
 Section near Old Peach Orchard, Ky 145 
 
 Section at Warfield, Ky., and on Tug Fork of Big Sandy River. .. 146 
 
 Section on Tug Fork of Big Sandy River, Logan Co., W. Va 147 
 
 Characteristic horizons 147 
 
 The Upper Freeport Coal 147 
 
 Section at McCoy Shaft, near Gallitzin, Cambria Co., Pa 148 
 
 Section near old Portage Railroad tunnel, at Gallitzin, Pa 149 
 
 Section at Mt. Equity mine, Bedford Co., Pa 149 
 
 Section at Posten’s bank, near Masontown, Preston Co., W. Va... 150 
 
 Section at Hartley’s bank, near Masontown, W. Va 150 
 
 Section at Wilson’s mine, Roaring Creek, Randolph Co.,W. Va .. 151 
 
 Section on Stone Coal Run, Upshur Co., W. Va 151 
 
 Section on the Buckhannon River, Upshur Co., W. Va 152 
 
 Section at Lloyd Wamsley’s bauk, Upshur Co., W. Va 152 
 
 Section at Bryan’s bank, Upshur Co., W. Va 152 
 
 Section at Current’s farm, Upshur Co., W. Va 152 
 
 Section near Hacker’s Valley post-office, Webster Co., W. Va 153 
 
 Section on the Little Kahawha River, Webster Co., W. Va 153 
 
 Section on the Holly River, Webster Co., W. Va 153 
 
 Section at Powell Mountain, Nicholas Co., W. Va 153 
 
 Section on Stroud Creek, Nicholas Co., W. Va 154 
 
 Sections on Mumble-the-Peg Creek, Nicholas Co., W. Va 154 
 
 Sections on the Guyandotte River, Cabell Co., W. Va 155 
 
 Sections on Cove Creek, Wayne Co., W. Va 155 
 
 Section on Twelve-pole Creek, Wayne Co., W. Va 156 
 
 Section on Little Laurel Creek, Wayne Co., W. Va 156 
 
 Section on Saw-pit branch of Cove Creek, Wayne Co., W. Va 157 
 
 Section in Sugar Camp Hollow, Wayne Co., W Va 157 
 
 Section on Trough Creek, Wayne Co., W. Va 157 
 
 Section at Greene Porter’s, Twelve-pole Creek, Wayne Co., W. Va. 158 
 
 Section near Kenova, W. Va 158 
 
 Section in Ritchie Co., W. Va 159 
 
 The Upper Freeport Limestone 159 
 
 The Bolivar Fireclay 159 
 
 The Upper Freeport Sandstone 160 
 
 The Middle Freeport Coal.. 160 
 
 The Lower Freeport Coal 160 
 
 Section near Philippi, Barbour Co., W. Va 161 
 
 Section of bed at Coalburg, Kanawha Co., W. Va 162 
 
 Section at Winifrede, Kanawha Co., W. Va 162 
 
 Section at mouth of Blaine Creek, Lawrence Co., Ky 162 
 
 The Lower Freeport Limestone 163 
 
 The Lower Freeport Sandstone 163 
 
 The Upper Kittauning Coal 164 
 
 The Johnstown (Cement) Limestone 165 
 
 The Middle Kittanning Coal 166 
 
 Section at Newburg, Preston Co., W. Va 167 
 
 Section in Hocking Valley, Ohio 168 
 
 Section at New Straits ville, Perry Co., Ohio 168 
 
 The Lower Kittanning Coal 169 
 
 Section at Newburg, Preston Co., W. Va 170 
 
10 CONTENTS. 
 
 Page. 
 
 Chap. V. The Lower Coal Measures, or Alleghany River Series — Continued. 
 
 The Kittanning Fire-clay 171 
 
 The Kittanning Sandstone 172 
 
 The Buhrstone Iron Ore 172 
 
 The Ferriferous Limestone 173 
 
 The Clarion Coal 175 
 
 Section near Eagle, Fayette Co., W. Va 176 
 
 The Eagle Limestone 177 
 
 The Brookville Coal 178 
 
 Chap. VI. The Pottsville Conglomerate Series 179 
 
 Thickness, character, and extents 179 . 
 
 Section in Fox Township, Elk Co., Pa 182 
 
 Section near Clearfield, Pa 182 
 
 Section at Brookville, Jefferson Co., Pa 183 
 
 Section at Patton Station, Red Bank Township, Clarion Co., Pa. 183 
 
 Section at Kellersburg, Armstrong Co., Pa 184 
 
 Section under Pittsburgh, Pa 184 
 
 Section under Murraysville, Pa 184 
 
 Section under Washington, Pa 185 
 
 Section in the Broad Top Basin, Huntingdon Co., Pa 185 
 
 Section near Wellersburg, Somerset Co., Pa 186 
 
 Section near Piedmont, Mineral Co., W. Va 186 
 
 Section on Black Fork of Cheat River, Tucker Co., W. Va 187 
 
 Section near Rowlesburgh, Preston Co., W. Va 188 
 
 Section near mouthy of Sandy Creek, Preston Co., W. Va 188 
 
 Section on Booth’s Creek, Taylor Co., W. Va 189 
 
 Section under Clarksburg, W. Va 189 
 
 Section near Farmington, W. Va 189 
 
 Section under Wellsburg, W. Va 190 
 
 Section in Mercer Co., Pa 190 
 
 Section near Quakertown, Mahoning Co., Ohio 191 
 
 Section in Holmes Co., Ohio 191 
 
 Section in Washington Co., Ohio 192 
 
 Section under Parkersburg, W. Va 192 
 
 Section near Burning Springs, Wirt Co., W. Va 192 
 
 Section at Jackson Furnace, Jackson Co., Ohio 193 
 
 Section at Hanging Rock, Scioto Co., Ohio 193 
 
 Section on Big Sandy River, at mouth of Blaine Creek 194 
 
 Section under Charleston, Kanawha Co., W. Va 195 
 
 Section at Burning Spring, Kanawha Co., W. Va 196 
 
 Section near Nuttallburg, Fayette Co., W. Va 167 
 
 Section on Crane Creek, Mercer Co., W. Va 198 
 
 Characteristic horizons 199 
 
 The Homewood Sandstone 199 
 
 The Mercer Group 200 
 
 The Connoquenessing Sandstones 201 
 
 The New River Coal Group 202 
 
 Section on Crane Creek, near Pocahontas, Va 203 
 
 Section at head of South Elk Horn Creek, McDowell Co., W. Val. 203 
 
 Section on East Branch of Simmon’s Creek, Mercer Co., W. Va 203 
 
 Section on Walker tract, Flipping Creek, Mercer Co., W. Va 204 
 
 Section on Pinnacle Fork of Guyaudotte River, Mercer Co., W. Va 204 
 
 The Sharon Conglomerate 204 
 
 The Lower Carboniferous Beds 205 
 
ILLUSTRATIONS. 
 
 Page. 
 
 Plate I. Map showing the general distribution of the Carboniferous in Penn- 
 sylvania, West Virginia, and Ohio Frontispiece. 
 
 II. Sections across the Appalachian Coal Fields. Figs. 1 and 2 16 
 
 III. Sections across the Appalachian Coal Fields, from Ravenna, Ohio, 
 
 to the Alleghany mountains 18 
 
 IV. Permo-Carboniferous, Cameron, W. Va 20 
 
 V. Upper Coal Measures, capped with Permo-Carboniferous beds, Wheel- 
 ing, W. Va 44 
 
 VI. Upper Coal Measures and Permo-Carboniferous, Powhatan, Ohio... 50 
 
 VII. Upper Coal Measures at Point Pleasant, W. Va 60 
 
 VIII. The Pittsburgh coal outcrop near Connellsville, Pa 64 
 
 IX. Lower Coal Measures, Coalburg, Kanawha River, W. Va 100 
 
 X. The Pottsville conglomerate topography in Blackwater Canyon 180 
 
 XI. The Pottsville conglomerate cliifs and d6bris, New River, West Vir- 
 ginia 202 
 
 Fig. 1. Section on Dunkard Creek, Greene Co., Pa 22 
 
 2. Section on Colvin’s Run, Greene Co., Pa 23 
 
 3. Section in Aleppo Township, Greene Co., Pa 24 
 
 4. Section at Board Tree, Marshall Co., W. Va 25 
 
 5. Section at Bellton, Marshall Co., W. Va 26 
 
 6. Section at New Martinsville, Wetzel Co., W. Va 27 
 
 7. Section at Baresville, Monroe Co., Ohio 28 
 
 8. Section in Liberty Township, Washington Co., Ohio 29 
 
 9. Section at Washington, Washington Co., Pa 29 
 
 10. Section near Taylorstown, Washington Co., Pa 30 
 
 , 11. Section in Fayette and Westmoreland Cos., Pa 44 
 
 12. Section at Brownsville, Fayette Co., Pa 44 
 
 33. Section at West Brownsville, Washington Co., Pa 45 
 
 14. Section at Rice’s Landing, Greene Co., Pa 45 
 
 15. Section on Robinson’s Run, Monongalia Co., W. Va 46 
 
 16. Section on Scott’s Run, Monongalia Co., W. Va 47 
 
 17. Section on Buffalo Creek, Marion Co., W. Va 48 
 
 18. Section at Clarksburg, Harrison Co., W. Va 49 
 
 19. Section on Chapline Hill, Wheeling, W. Va 49 
 
 20. Section near Bellaire, Ohio 50 
 
 21. Section at Moundsville, W. Va 51 
 
 22. Section on Pipe Creek, Belmont Co., Ohio 51 
 
 23. Section in Washington Co., Ohio 52 
 
 24. Section at Burning Springs, Wirt Co., W. Va 52 
 
 25. Section on Leading Creek, Gilmer Co., W. Va . ... 53 
 
 26. Section at Antique, Meigs Co., Ohio : 53 
 
 27. Section at Hartford City, Mason Co., W. Va 54 
 
 28. Section at Arbuckle, Mason Co., W. Va 54 
 
 11 
 
12 
 
 LIST OP ILLUSTRATIONS. 
 
 Fig. 29. Section at month of Big Hurricane Creek, Putnam Co., W. Va 
 
 30. Section opposite Winfield, Putnam Co., W. Va 
 
 31. Section n^ar Raymond City, W. Va P - 
 
 32. Section in vicinity of Westernport, Md ... 
 
 33. Section in the Pittsburgh region '.... 
 
 34. Section at Sewickley, Fa 
 
 35. Section on Dunbar Creek, Fayette Co., Pa w 
 
 36. Section at Ligonier, Westmoreland Co., Pa 
 
 37. Section in vicinity of Berlin, Somerset Co., Pa 
 
 38. Section at Broad Top, Bedford Co., Pa 
 
 39. Section opposite Steubenville, Ohio 
 
 40. Section at Washington, Pa 
 
 41. Section near Cannonsburg, Washington Co., Pa 
 
 42. Section at Morgantown, W. Va 
 
 43. Section at Little Falls, Monongalia Co., W. Va 
 
 44. Section at Newburg, Preston Co., W. Va 
 
 45. Section at Fairfax Knob, Tucker Co., W. Va 
 
 46. Section in Guernsey Co., Ohio 
 
 47. Section at Burning Springs, Wirt Co., W. Va 
 
 48. Section near Huntington, W. Va 
 
 49. Section near Charleston, W. Va 
 
 50. Section at Blossburg, Tioga Co., Pa 
 
 51. Section at Fall Brook, Tioga Co., Pa 
 
 52. Section at Karthaus, Clearfield Co., Pa. 
 
 53. Section in Horton Township, Elk Co., Pa 
 
 54. Section at Brock way ville, Jefferson Co., Pa 
 
 55. Section in Clarion Co., Pa 
 
 56. Section at Miller’s Eddy, Clarion Co., Pa ... 
 
 57. Section at East Brady, Clarion Co., Pa 
 
 58. Section near New Bethlehem, Clarion Co., Pa 
 
 59. Section in Brady Township, Butler Co., Pa 
 
 60. Section near Ore Hill Furnace, Armstrong Co., Pa 
 
 61. Section at Centerville, Armstrong Co., Pa 
 
 62. Section at Putney ville, Armstrong Co., Pa 
 
 63. Section near Kittanning, Pa 
 
 64. Section 5 miles below Kittanning, Pa : 
 
 65. Section at Logansport, Armstrong Co., Pa 
 
 66. Section at Freeport, Pa 
 
 67. Section near mouth of Beaver River, Pa 
 
 68. Section at Sewickley, Allegheny Co., Pa 
 
 69. Section under Washington, Pa 
 
 70. Section near Carpenter’s Station, Westmoreland Co., Pa 
 
 71. Section under Murraysville, Westmoreland Co., Pa 
 
 72. Section on Beaver Run, Westmoreland Co., Pa 
 
 73. Section near Richmond, Indiana Co., Pa 
 
 74. Section near Lockport and Bolivar, Indiana Co., Pa 
 
 75. Section on Laurel Run, near Laughlintown, Westmoreland Co., Pa .. 
 
 76. Section on Cucumber Run, Stewart Township, Fayette Co., Pa 
 
 77. Section at Newburg, Preston Co., W. Va 
 
 78. Section at Johnstown, Cambria Co., Pa 
 
 79. Section at Conemaugu, near Johnstown, Pa . . ' 
 
 80. Section in Jackson Township, Cambria Co., Pa.. 
 
 81. Section on Ben’s Creek, Cambria Co., Pa 
 
 82. Section near Stoyestown, Somerset Co., Pa 
 
 83. Section at Pinkerton Point, Somerset Co., Pa 
 
 Page. 
 
 55 
 
 55 
 
 56 
 56 
 
 72 
 
 73 
 
 74 
 
 75 
 
 76 
 
 77 
 
 77 
 
 78 
 
 78 
 
 79 
 
 80 
 81 
 82 
 83 
 
 83 
 
 84 
 
 85 
 1(2 
 103 
 
 103 
 
 104 
 
 104 
 
 105 
 
 105 
 
 106 
 106 
 107 
 
 107 
 
 108 
 108 
 109 
 
 109 
 
 110 
 111 
 112 ’ 
 112 
 113 
 
 113 
 
 114 
 
 114 
 
 115 
 
 115 
 
 116 
 116 
 
 117 
 
 118 
 119 
 
 119 
 
 120 
 121 
 121 
 
LIST OF ILLUSTRATIONS. 13 
 
 Page. 
 
 Fig. 84. Section at Cresson, Pa 122 
 
 85. Section at Bennington, Blair Co., Pa 122 
 
 86. Section at Clearfield, Clearfield Co., Pa 123 
 
 87. Section near Morriedale, Clearfield Co., Pa 123 
 
 88. Section at Sterling mines, near Houtzdale, Clearfield Co., Pa 124 
 
 89. Section on Shoup’s Run, Broad Top Basin, Huntingdon Co., Pa 125 
 
 90. Section East Broad Top Basin, Huntingdon Co., Pa 125 
 
 91. Section in Broad Top Basin, Bedford Co., Pa 126 
 
 92. Section at Piedmont, Mineral Co., W. Ya 126 
 
 93. Section on North Potomac, at Maple Swamp Water Tank, West Vir- 
 
 ginia Central Railroad 127 
 
 94. Section near Thomas, Tucker Co., W. Va 127 
 
 95. Section near Moatsville, Barbour Co., W. Ya 128 
 
 96. Section at Valley Falls, Taylor Co., W. Va.. 128 
 
 97. Section near Nuzum’s Mills, Marion Co., W. Va 129 
 
 98. Section under Clarksburg, W. Va 129 
 
 99. Section under Parkersburgh, W. Va 130 
 
 100. Section under Wheeling, W. Va 130 
 
 101. Section at mouth of Little Beaver, on the Ohio-Pennsylvania line 130 
 
 102. Section near Sprucevale, Columbiana Co., Ohio 131 
 
 103. Section between New Lisbon and Leetonia, Ohio 132 
 
 104. Section at Zanesville, Muskingum Co., Ohio 132 
 
 105. Section in vicinity of Shawnee and McCuneville, Perry Co., Ohio... 133 
 
 106. Section in Hocking Valley, near Buchtel, Ohio 133 
 
 107. Section on Meeker’s Run, near Nelsonville, Athens Co., Ohio 134 
 
 108. Section in Panther Hill, Mt. Vernon Furnace, Scioto Co., Ohio 134 
 
 109. Section at Ironton, Ohio 135 
 
 110. Section in southern Ohio, above Ironton ^ 135 
 
 111. Section under Charleston, W. Va 136 
 
 112. Section at mouth of Lick Run, 2 miles above Charleston, W. Va 137 
 
 113. Section at Dickinson salt works, Kanawha Co., W. Va 138 
 
 114. Section near Brownstown, 3 miles south from Malden 139 
 
 115. Section at mouth of Armstrong Creek, on the Big Kanawha River... 140 
 
 116. Section at Guyandotte Mountain, Raleigh Co., W. Va 142 
 
 117. Section near Oceana, Wyoming Co., W. Va 143 
 
 118. Section at mouth of Blaine Creek, 20 miles above mouth of Big 
 
 Sandy River, Lawrence Co., Ky 144 
 
 119. Section near Peach Orchard, Lawrence Co., Ky 145 
 
 120. Section near Warfield, Ky., on Tug Fork of Big Sandy River 146 
 
 121. Section on Tug Fork of Big Sandy River, near mouth of Knox Creek, 
 
 southern edge of Logan Co., W. Va 147 
 
 122. Section in Fox Township, Elk Co., Pa 182 
 
 123. Section at Clearfield, Pa 183 
 
 124. Section at Brookville, Jefferson Co., Pa 183 
 
 125. Section at Patton Station, Red Bank Township, Clarion Co., Pa ... 183 
 
 126. Section at Kellersburgh, Armstrong Co., Pa 184 
 
 127. Section under Pittsburgh, Pa 184 
 
 128. Section under Murray sville, Pa 185 
 
 129. Section under Washington, Pa 185 
 
 130. Section in the Broad Top Basin, Huntingdon Co., Pa 185 
 
 131. Section on Gladden’s Run, near Wellersburg, Somerset Co., Pa 186 
 
 132. Section near Piedmont, Mineral Co., W. Va 186 
 
 133. Section on Black Fork of Cheat River, Tucker Co., W. Va 187 
 
 134. Section along the Baltimore and Ohio Railroad, Cheat River grade, 
 
 4 miles west from Rowlesburgh, Preston Co., W. Va 188 
 
‘ 
 
 14 LIST OF ILLUSTRATIONS. 
 
 Page. 
 
 Fig. 135. Section near mouth of Sandy Creek, Cheat River, Preston Co., W.Va ... 188 
 
 136. Section on Booth’s Creek, Taylor Co., W.Ya 189 
 
 137. Section under Clarksburg, W. Ya 189 
 
 138. Section near Farmington, W. Va 189 
 
 139. Section under Wellsburgh, W. Ya 190 
 
 140. Section in Mercer Co., Pa 190 
 
 141. Section at Ohio and Pennsylvania line, on Mahoning River 191 
 
 142. Section in Holmes Co., Ohio 191 
 
 143. Section of Epler oil boring, Washington Co., Ohio 192 
 
 144. Section under Parkersburg, W. Ya 192 
 
 145. Section at Simpson Well, Wirt Co., W.Ya 192 
 
 146. Section at Jackson Furnace, Jackson Co., Ohio 193 
 
 147. Section at Hanging Rock, Scioto Co., Ohio 193 
 
 148. Section under Big Sandy River, at mouth of Blaine Creek 194 
 
 149. Section under Charleston, Kanawha Co., W. Va 195 
 
 150. Section at Burning Spring, Kanawha Co.. W. Ya 196 
 
 151. Section in vicinity of Nuttallburgh, Fayette Co., W. Ya 197 
 
 152. Section on Crane Creek, Mercer Co., W. Va 198 
 
LETTER OF TRANSMITTAL. 
 
 Department of the Interior, 
 
 U . S. Geological Survey, 
 
 Appalachian Division, 
 Morgantown , W. Va ., July 15, 1890. 
 
 Sir: I have the honor to transmit herewith the results of my study 
 of the stratigraphy of the bituminous coal rocks in the northern half 
 of the Appalachian field. 
 
 As stated in the body of this report, it can not be expected that this 
 first attempt to correlate the different beds of coal, limestone, and sand- 
 stone over such a wide area will be free from error, but it represents * 
 my best efforts to harmonize the strata of the several regions. No 
 one knows better than 1 that many of the identifications suggested are 
 largely preliminary, and I not only expect but request the friendly 
 criticism of my brother geologists, knowing that all will be pleased 
 when the correct order of these interesting deposits shall be finally 
 determined. 
 
 Many questions of great geological interest have not been discussed 
 in this report, for the reason that I thought it best to postpone their 
 treatment until some one should have done for the southern half of the 
 Appalachian coal field what I have attempted for the northern half, 
 since the field is a unit from Pennsylvania to Alabama, and in the dis- 
 cussion should be treated as such. 
 
 It is hardly necessary to say that the accompanying map is not pre- 
 sented with any claim for accuracy as to details, but only to show in a 
 rough way the general distribution of the different members, and with 
 the hope that it may prove of some service in the preparation of a cor- 
 rect map of these several series when the Survey shall have extended 
 "ts topographic work over the entire region. 
 
 Very respectfully, your obedient servant, 
 
 I. C. White. 
 
 Hon. J. W. Powell, 
 
 Director U. S. Geological Survey , Washington , D. C. 
 
 15 
 
/ 
 
 
 
 
 
 / 
 
 
 
 
 
 
 
 
 
 
 
 
 K 
 
 
 
Fig. 2 
 
 izontal Scale 36oooFT=I inch, 
 vtical ” 36 oo ” 
 
 ONS ACROSS THE APPALACHIAN COAL FIELDS. 
 
 , to the eastern edge of the Alleghany Mountains. 
 
 ihow the thickening of the several coal groups between Jackson County, Ohio, and Fayette County. West 
 
I MILLERSBURG. 
 
 CONG^JMEASURES 
 
 SmLeVcZ. 
 
 M E A S U 
 
 UPPER COAL MEASURES. 
 
 PERMO-CARB. MEASURES. 
 
 m 
 
 PERMO-CARB. measures 
 
 Fig. Z. 
 
 Horizontal Scale 36oooFT=I inch, 
 Vertical " 36 oo ” 
 
 SECTIONS ACROSS THE APPALACHIAN COAL FIELDS. 
 
 ?, Ohio, to the eastern edge of the Alleghany Mountains. 
 
 veen Jackson County, Ohio, and Fayette County. West 'irginia. 
 
STRATIGRAPHY OF THE BITUMINOUS COAL FIELD 
 IN PENNSYLVANIA, OHIO, AND WEST VIRGINIA. 
 
 By I. C. White. 
 
 CHAPTER I. 
 
 AREA, STRUCTURE, AND CLASSIFICATION. 
 
 The Appalachian Basin contains the largest continuous coal field of 
 any Carboniferous area. Beginniug near the northern line of Pennsyl- 
 vania, latitude 42°, longitude 77°, it extends southwestward through 
 TVest Virginia, southeastern Ohio, eastern Kentucky, and central Ten- 
 nessee, ending in western Alabama, latitude 33°, longitude 88°, 900 
 miles from its northern terminus. 
 
 The shape of the field has been compared to that of a rude canoe 
 the poiu ted ends being in Pennsylvania and Alabama, respectively, while 
 the broadest portion lies in southern West Virginia and Ohio. 
 
 As is well known, the general structure of the field is that of a great 
 trough or basin, the line of greatest depth leaving Pennsylvania near 
 its southwest corner, and passing down through West Virginia rudely 
 parallel to the Ohio River, to enter Kentucky 10 miles above the mouth 
 of the Big Sandy River. This general trough or geo-syncline is itself 
 traversed, especially in its northeastern portion, by a series of flexures 
 which, although so gentle along the region west of the center of the 
 field as to be recognizable with difficulty, yet eastward thereof they 
 increase in amplitude until the great folds of the Alleghany Mountains 
 become a part of the system. 
 
 The map sections shown on Pis. X and XI, crossing the Appalachian 
 held nearly normal to the strike, will give the reader a good idea of the 
 structure of the northern half of this field at the localities indicated on 
 the map (PI. I), and they also show how the folds which are so promi- 
 nent at the northeast gradually die out toward the southwest, so that 
 in the region ot the Great Kanawha River they almost disappear. This 
 flattening out of the flexures in southern West Virgiuia has been 
 ascribed by Professors Fontaine and Stevenson to the development of 
 the great system of faults along the southeastern margin of the coal field 
 m the edge of Virginia, whicU relieved the teusiou ou the rocks over 
 Bull, 65 — 3 17 
 
18 THE NORTHERN BITUMINOUS COAL FIELD. [buu.65. 
 
 the adjoining portion of the Appalachian field and thus prevented their 
 folding as in Pennsylvania and northern West Virginia. These anti- 
 clinal and synclinal folds so well developed at the north are nearly par- 
 allel .to the Alleghany Mountains, but as they begin to die away in 
 central West Virginia a large anticline (the Volcano) runs nearly north 
 and south diagonally across the general strike of the beds. 
 
 There are probably other folds in the southwestern part of West Vir- 
 ginia, which, like the Volcano anticline, run contrary to the usual direc- 
 tion, but they have not been traced out with sufficient care to warrant 
 description. 
 
 The distribution of the different geological groups on the accompany- 
 ing map will serve to show the general position and direction of the 
 principal anticlines, but the topographic base of the map is so inaccu- 
 rate that it was thought best not to attempt to put in the anticlinal 
 lines of the region described till the Survey should have completed the 
 regular topographical map. 
 
 In this connection it should be stated that this map is not presented 
 with any claims for accuracy in detail, but simply to show the general 
 distribution of the Carboniferous system. 
 
 The portion of the Appalachian region herein described includes only 
 the bituminous coal fields of Pennsylvania, Ohio, and West Virginia. 
 
 The Pennsylvania and Virginia geologists, led by the two illustrious 
 Rogers brothers, long ago discovered that the main coal-bearing portion 
 of the Carboniferous system could be naturally subdivided into five 
 series. This generalization was founded upon a careful study of the 
 rocks over a wide area, and the subsequent work of other geologists has 
 fully established its general truthfulness to nature as well as its great 
 usefulness in stratigraphic geology. 
 
 The more detailed and minute studies of recent years, rendered 
 possible by vast mining developments, have only modified the Rogers 
 classification, and hence it has become so thoroughly ingrafted into 
 geological nomenclature and so familiar to the minds of practical coal 
 operators that it would be very unwise to make any radical changes in it. 
 It is true that in minor details the original nomenclature for some of 
 these series was misleading, but this does not materially affect the grand 
 truths expressed in the general framework of the classification, and 
 hence it has been deemed best to modify and supplement this time- 
 honored work, rather than to destroy it and cast it away, as has recently 
 been suggested by some geologists. 
 
 The classification adopted in this report attempts to preserve what- 
 ever of the old nomenclature has been found useful and helpful to 
 geologists, while at the same time such new features are introduced as 
 seem necessary from our wider and more intimate knowledge of these 
 
 rocks. J 
 
 The entire Carboniferous system of the Appalachian region subdivides! 
 naturally into three grand divisions fouuded upon conditions of accu*J 
 
• HARMARVILLE RO 
 I ALLEGHANY RIVER 
 
 
 Horizontal Scale 5 Miles= I inch. 
 Vertical »5oooFT » » 
 
 SECTION ACROSS THE APPALACHIAN COAL FIELDS, FRO»< RAVENNA, OHIO, TO THE ALLEGHANY MOUNTAINS. 
 
 
WHITE.] 
 
 DIVISIONS OF THE -CARBONIFEROUS SYSTEM. 
 
 19 
 
 mulation, and these in turn split up into eight minor series, as exhibited 
 in the following scheme : 
 
 Divisions. 
 
 Upper: fresh and 
 brackish water 
 deposits. 
 
 Carboniferous ^ Middle: shore de- 
 fcYSTEM posits, with in- 
 
 cursions of the 
 
 Lower: in arine 
 deposits. 
 
 Series. 
 
 Permo-Carboniferous, No. XYI, Dunkard Creek Series. 
 
 Upper Coal Measures, No. XV, Monongaliela River Series. 
 
 Upper half. 
 
 Barren Measures, No. XIV, Elk River Series. 
 
 Lower half. 
 
 Lower Coal Measures, No. XIII, Allegheny River Series. 
 
 Pottsville Conglomerate Measures, “Great,” “Serai,” No. XII, 
 Conglomerate, etc. 
 
 Mauch Chunk Red Shale, Umbral Red Shale. 'i 
 
 Mountain Limestoue, Umbral Limestone, Green- >No. XI. 
 brier, etc. ) 
 
 Pocono Sandstone, Vespertine, No. X, “Big Injun ” oil sand, etc. 
 
 As will be seen from the foregoing diagram, the line between the 
 Middle and Upper Carboniferous deposits passes directly through the 
 center of the Elk Biver series. This is due to the fact that marine 
 conditions ceased, never to return, with, the deposition of the Crinoidal 
 limestone and its associated beds, midway in the Barren Measures, 
 thus separating them into two divisions which are of almost equal thick- 
 ness, the lower one abounding in marine life, while the upper has nothing 
 but fresh or brackish water forms. The change in this respect is great 
 enough to warrant the separation of the Barrens into two series, but as 
 the lithological differences at the line of separation are very meager, it 
 is deemed best to keep these rocks a unit as in the Bogers nomenclature. 
 
 This report deals only with the Middle and Upper Carboniferous of 
 the above table, and the five series into which they are subdivided will 
 now be described in detail, beginning with the highest. 
 
 The discussion of many interesting questions connected with Carbon- 
 iferous geology is necessarily postponed until the rest or southern half 
 of the Appalachian coal field has been carefully studied as a whole. 
 
CHAPTER II. 
 
 THE PERMO-CARBONIFEROUS OR DUNKARD CREEK SERIES. 
 
 THICKNESS, CHARACTER, AND EXTENT. 
 
 The rocks of this series (Upper Barren Measures, No. XVI) begin with 
 the roof shales of the Waynesburg coal and exteud upward to the top- 
 most beds of the Appalachian region. 
 
 How many feet of deposits erosion has removed above the highest 
 remaining beds we can only conjecture. However, if the soft and easily 
 yielding character of the rocks which have escaped disintegration can 
 be taken as a criterion for those that have wasted away, the thickness 
 of the latter must be reckoned by the thousand and probably by the 
 10,000 feet. 
 
 Several independent measurements from the highest accessible sum- 
 mits foot up a little more than 1,150 feet for the thickness of the series 
 and it is certain that no other localities could exceed this by more than 
 100 feet. 
 
 The uppermost beds are found at the headwaters of Dunkard Creek, 
 a large stream which heads near the West Virginia-Pennsylvania line, 
 on the eastern slope of the watershed separating the Ohio and Mono*n- 
 gahela River drainage system, and flowing eastward puts into the 
 Monougahela two miles above Greensboro, Greene County, Pennsyl- 
 vania, and four miles north from the West Virginia line. This stream 
 flows over Permo-Carboniferous rocks from its source to the point at 
 which it leaves the West Virginia line at Mount Morris, Pennsylvania, 
 a distauce of more than thirty miles, furnishing very fine exposures of 
 these rocks along its banks and bluffs; hence the geographical name 
 (Dunkard Creek) which I have given the series. 
 
 These deposits occupy a rather limited area in the Appalachian field, 
 being found in only two counties (Greene and Washington) of Pennsyl- 
 vania, with the exception of small isolated patches in Fayette, West- 
 moreland, and Allegheny. In Ohio there is a larger area of them 
 bordering the Ohio River through the counties of Belmont, Monroe, 
 Washington, Athens, Meigs, and Gallia. But it is in West Virginia 
 that we find the principal belt of these beds, for there they cover a wide 
 20 
 
5EOLOGICAL SURVEY 
 
 PERMO-CARBONIFEROUS, CAMERON, WEST VIRGINIA. 
 
Of wt 
 
 WWttW' 
 
 Of ILUHUVS 
 
WHITE.] 
 
 CHARACTER OF THE DUNKARD CREEK SERIES. 
 
 21 
 
 region bordering the Ohio River between the Pennsylvania line at the 
 north and the Great Kanawha River on the south, as the accompanying 
 map shows. 
 
 The character of the rocks varies greatly in different portions of this 
 area. At the northeastern end of the field, in Washington County, 
 Pennsylvania, limestones seem to predominate in thickness over the 
 gray shales, sandstones, and thin coal beds with which they are there 
 interstratitied. But south westward the limestones and coals gradually 
 disappear, so that in Jackson County, West Virginia, no regular coal 
 beds are found, and only one limestone (the Nineveh) remains. The 
 limestones continue in considerable number in Greene, Ohio, Marshall, 
 and Monongalia Counties, and the northern part of Wetzel County, but 
 southward from this line they rapidly disappear, with the single excep- 
 tion noted. The coal beds all die out with the disappearance of the 
 limestones, except one (the Washington), which seems to extend beyond 
 the Little Kanawha River before it passes out of the series. 
 
 As the limestones and thin coal beds gradually fade out to the south- 
 west, red shale, a variety of rock almost unknown in Washington County, 
 Pennsylvania, gradually comes into the section in thin beds at first, but 
 finally extends throughout the whole series, and forms nearly one-half 
 its thickness, thus making a broad band of red soil from the Pennsyl- 
 vania line southwestward to the Great Kanawha River. 
 
 This increase in red shale beds is accompanied by an increase in the 
 number and massiveness of the sandstone rocks, so that the topography 
 gradually becomes greatly different from that found in Washington 
 County, Pennsylvania. There the surface is gently rolling, the valleys 
 broad, and the hills rounded, with no deep gorges or precipitous slopes, 
 the abundance of limestone rendering the soil so highly fertile that the 
 region has long been famed as one of the finest grazing and agricultural 
 districts in the Union. But toward the southwest, while the soil remains 
 very fertile, owing to a large quantity of marly material in the red 
 shales, yet the thickening up of the sandstone beds makes the valleys 
 narrow and the lower portion of the hills often precipitous, the arable 
 land being confined largely to the ridges, so that the soil is better 
 adapted to grazing than tillage. In many cases the massive sandstones 
 crop out along the ridges which they have protected from erosion, 
 forming narrow “ hogbacks,” from which the surface falls away rapidly 
 on each side. Another peculiarity of these beds is that the sand rocks 
 contain no pebbles except near the base of the series, since above the 
 Way nesburg sandstone no pebbles larger than coarse sand grains have 
 ever been seen by the writer in all of the 1,000 feet of deposits, except 
 at a single locality on the Parkersburg and Staunton turnpike, along 
 the dividing ridge between Ritchie and Gilmer Counties, West Virginia, 
 where locally the Marietta Sandstones, 140 feet above the Washington 
 coal, thicken up into a very coarse conglomerate, filled with quartz 
 pebbles. 
 
1BE3HI 
 
 22 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL? 65. 
 
 The character of the rocks which compose these measures in the sev- 
 eral regions of their area will be seen from the sections 
 which follow. 
 
 Section on Dunkard Creek , Greene County , Pennsyl- 
 vania. — Fig. 1 shows the succession found along Dunkard 
 Greek, from £lie head of its Pennsylvania fork in Gil- 
 more Township, Greene County, eastward to where the 
 stream veers northward back into Pennsylvania at 
 Mount Morris. 
 
 Dunkard Creek, Greene County, Pennsylvania. 
 
 I00 - 
 
 [See map, L 1 to L Is.] 
 
 Ft. in. 
 
 1. Concealed from top of Shough’s 
 
 knob 165 
 
 2. Sandstone, massive, Gilmore 40 
 
 3. Shales, with limestone at base ... 15 
 
 4. Sandstone and shales and con- 
 
 cealed 100 
 
 5. Shale, red 2 
 
 6. Shales, gray 20 
 
 7. Shale, marly 2 
 
 8. Sandstone aud shale. 35 
 
 9. Shale, red 3 
 
 10. Sandstone and shale 50 
 
 11. Red shale 3 
 
 12. Shales aud sandstone, Nineveh.. 25 
 
 13. Shales . 20 
 
 14. Coal, Nineveh 1 6 
 
 15. Shales 28 
 
 16. Limestone (No. X), Nineveh 7 
 
 17. shales, sandstone and concealed. 100 
 
 18. Sandstone, massive. FishCreet.. 20 
 
 19. Shales with fossil plants 10 
 
 t Joal. . 0-' 5" ) 
 
 20. Coal, Dunkard. < Slate O' 1" > .. 1 
 
 ( Coal.. 0' 6" ) 
 
 21. Limestone 1 
 
 •22. Sandstone 10 
 
 23. Shales 17 
 
 24. Limestone, Jolly town 1 6 
 
 25. Shales and sandstone 25 
 
 26. Coal, Jolly town 1 1 
 
 27. Calcareous shale, fossiliferous, 
 
 fish teeth 0 6 
 
 28. Limestone. Upper Washington .. 4 
 
 29. Shales and sandstone 115 
 
 30. Limestone, Middle Washington.. 3 
 
 31. Shales 40 
 
 32. Sandstone 35 
 
 33. Shale... 5 
 
 Cool Wash (Coal, impure. V 2") 
 
 31- . A F're clay .... 2' 6"> 4 
 
 ington A. } C()al ._/ o'6"$ 
 
 35. Shales and sandstones 60 
 
 36. Limestone, Lower Washington .. 5 
 
 37. Shales 5 
 
 38. Coal, Washington, slaty 5 
 
 39. Shales and sandstones, including 
 
 a coal bed near center 110 
 
 40. Coal, Waynesburg, “A’’. 2 
 
 41. Shales 10 
 
 42. Sandstone, Waynesburg 50 
 
 43. Shales, with fossil plants (Cass- 
 
 ville) 5 
 
 44. Waynesburg coal. 
 
 > 
 
 > 
 
 ) 
 
 K 
 
 ) 
 
 ) 
 
 Ft. in. 
 
 480 
 
 223 
 
 276 8 
 
 182 6 
 
 Total 
 
 1,162 3 
 
 Fig. 1.— Section on Dunkard Creek, Pa. 
 
WHITE. ] 
 
 SECTION ON COLVIN S HUN, PENNSYLVANIA. 
 
 23 
 
 Section on Colvin’s Run , Greene County , Pennsylvania . — The lower half 
 of this Dunkard Creek series is very finely exposed in a continuous sec- 
 tion on Colvin’s Run, a tributary of Dunkard which empties into it near 
 Mount Morris, Greene County, Pennsylvania, and in descending this 
 stream the following intervals, as shown in Fig. 2, were carefully meas- 
 ured : 
 
 
 
 Ft. in. 
 
 > 190 6 
 
 }■ 245 
 
 I 
 
 Colvin’s Bun, Greene County, Pennsylvania. 
 
 [See map, L 1.] 
 
 Ft. in. 
 
 1. Limestone, Nineveh 9 
 
 2. Shales and sandstone 135 
 
 3. Limestone, Jolly town 10 
 
 4. Sandy shales 35 
 
 5. Coal, Jollytown 1 6 
 
 6. Shales, sandy 35 
 
 7. Sandstone, massive 15 
 
 8. Sandy shales and concealed 40 
 
 9. Red shales 10 
 
 10. Shales 25 
 
 11. Sandstone 10 
 
 12. Shales 15 
 
 13. Coaly shales, Washington, “A” 2 
 
 14. Sandy shales and sandstone 45 
 
 15. Limestone, gray , 2 
 
 16. Shales 5 
 
 17. Sandstone, massive 15 
 
 18. Shales 15 
 
 19. Limestone, Washington Lower 7 
 
 20. Shale, dark 4 
 
 21. Coal, Washington 2 6 
 
 22. Shales and sandstone 45 
 
 23. Coal, Waynesburg, “B’’ 2 
 
 24. Shales and sandstone 35 
 
 25. Limestone, Colvin’s Run 3 
 
 26. Shales 1 
 
 27. Coal, Waynesburg, “A” 2 
 
 28. Limestone 2 
 
 29. Shales 5 
 
 30. Sandstone, Waynesburg I 75 
 
 31. Shales, with fossil plants (Cassville) 5 
 
 32. Coal, Waynesburg. 
 
 Total 613 
 
 > 177 6 
 
 Fig. 2. — Section on Col- 
 vin’s Run, Pa. 
 
24 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65. 
 
 Section in Aleppo Township , Greene County, Pennsylvania . — Wheeling 
 Creek rises on the western slope of the Monougahela-Ohio divide, and 
 flowing westward enters the Ohio River at Wheeling. 
 It furnishes excellent exposures of the Dunkard beds 
 from the summit of the series to the base. The follow- 
 ing intervals (Fig. 3) were measured along the Dunkard 
 Fork of the creek between its source in Aleppo Town- 
 ship, Greene County, Pennsylvania, and the mouth of 
 Crab Apple Creek, near the West Virginia line: 
 
 
 60' 
 
 
 30 t 
 
 wmm * 
 
 
 Z!f 
 
 
 
 pwi 
 
 IS' 
 
 
 
 
 
 
 
 — — 
 
 6' 
 
 
 40' 
 
 
 
 1=:=.^= = = 
 
 gggggggj 
 
 60’ 
 
 
 
 
 10’ 
 
 
 25* 
 
 •Xv.V.v.v.v. 
 
 
 mmWM 
 
 65’ 
 
 
 
 
 
 54 
 
 ,( 
 
 HOT 
 
 vt 
 
 - ==J 
 
 10' 
 
 
 45' 
 
 
 
 Aleppo Township , Greene County , Pennsylvania. 
 
 [See map, L j.] 
 
 Ft. in. 
 
 1. Shales and sandstones 60 
 
 2. Limestone, Windy Gap 4 
 
 3. Shale 25 
 
 4. Coal and bituminous shale. 
 
 Windy Gap 2 
 
 5. Shale 30 
 
 6. Sandstone, Gilmore 30 
 
 7. Concealed (shales, sandstones, 
 
 and limestones) 300 
 
 8. Coal, Nineveh 1 
 
 9. Shales 25 
 
 10. Limestone, Xineveh 8 
 
 11. Shales and sandstone 40 
 
 12. Coal 1 2 
 
 13. Limestone 2 
 
 14. Sandstone 30 
 
 15. Limestone 8 
 
 16. Shales and sandstone 70 
 
 17. Limestone 2 
 
 18. Shale 15 
 
 19. Coal, Dunkard 2 
 
 20. Limestone 1 6 
 
 21. Shaly sandstone 25 
 
 22. Limestone, Jollytown 2 
 
 23. Shales and sandstone 115 
 
 24. Dark, calcareous shale 2 
 
 25. Limestone 6 
 
 26. Shales and sandstone 40 
 
 27. Limestone 2 
 
 28. Shales and sandstone 60 
 
 29. Shales 10 
 
 30. Sandstone 25 
 
 31. Shales, sandstones, and con- 
 
 cealed 66 
 
 32. Coal, Washington 4 
 
 33. Shales and concealed. 54 
 
 34. Coal, Waynesburg, “B” 1 
 
 35. Shales 24 
 
 36. Coal, W ay nesburg, “ A ’ ’ 0 
 
 37. Shales 10 
 
 38. Sandstone, Waynesburg 45 
 
 39. Coal, Waynesburg. 
 
 Total 
 
 Ft. in. 
 
 451 
 
 } 232 8 
 
 326 
 
 ]■ 138 
 
 1,147 8 
 
 Fig. 3. —Section in Greene County, Pa. 
 
WHITE. 1 
 
 SECTION AT BOARD TREE, WEST VIRGINIA. 
 
 25 
 
 3!j 
 
 Section at Board Tree Tunnel , Marshall County , West Virginia . — At 
 Board Tree Tunnel, on the Baltimore and Ohio Bailroad, and close to 
 the line between Wetzel and Marshall Counties, some 
 very high land occurs, while an oil well boring in the 
 valley of Fish Creek near by carries the rock meas- 
 urement down to the base of the Dunkard Creek beds. 
 In descending from Bice’s Knob past the western por- 
 tal of Board Tree Tunnel to the Kuce farm oil boring 
 ' on Fish Creek, and connecting with the record of the 
 latter, the following succession (Fig. 4) is revealed : 
 
 Board Tree. Marshall County , West Virginia. 
 
 t?. : v iv.-::-:; 
 
 is* 
 
 100 ’ 
 
 AOf 
 
 26 1’ 
 
 [See map, L j.] 
 
 1. Sandstone, gray, and concealed*. 
 
 2. Gray limestone, Windy Gap 
 
 3. Red shales and concealed 
 
 4. Coaly slate 
 
 5. Concealed to base of a massive 
 
 sandstone 
 
 6. Concealed, sandstone and red 
 
 shale to Board Tree Tunnel 
 
 7. Sandy shales 
 
 8. Sandstone, Nineveh 
 
 9. Coal, Nineveh 
 
 10. Gray shales 
 
 11. Sandstone, massive 
 
 12. Shales 
 
 1'1 
 
 13. 
 
 150 
 
 [Limestone 
 
 C Limestone ! Black slate . 
 
 \ Nineveh . ; Limestone and 
 limy beds 
 
 14. Variegated shales 
 
 15. Sandstone 
 
 16. Shales, limy 
 
 17. Sandstone, to level o£ track at 
 
 west portal 
 
 18. Concealed shales and sandstone. 
 
 19. Massive sandstone, Fish Creek. 
 
 20. Shales 
 
 21. Coal, Dunkard, to level of bore 
 
 hole 
 
 22. Interval, shales, sandstones, and 
 
 limestones, with two thin coal 
 beds 
 
 23. Shales, sandstones, and red beds. 
 
 24. Coal, Washington 
 
 25. Shales, limestones, and sandstone. 
 
 26. Coal, Wayneshurg. 
 
 Ft. 
 
 55 
 
 5 
 
 100 
 
 1 
 
 35 
 
 175 
 
 15 
 
 15 
 
 1 
 
 15 
 
 12 
 
 3 
 
 19 
 
 9 
 
 5 
 
 7 
 
 100 
 
 30 
 
 3 
 
 50 
 
 150 
 
 Ft. 
 
 401 
 
 } 261 
 
 300 
 
 155 
 
 15!? 
 
 Total 
 
 1,117 
 
 There is some uncertainty about the 
 horizon of the Pittsburgh coal in the 
 oil boring, since two large beds are re- 
 ported, one at 700 feet and the other 
 at 800. The latter is the thicker bed, 
 and as the depth from it to the third oil sand (2,100 feet) agrees with the 
 
 Fig. 4. — Section at Board Tree Tunnel, Mar- 
 shall Comity, W. Va. 
 
26 
 
 THE NORTHERN BITUMINOUS COAL FIELD, 
 
 [bull. 65. 
 
 same interval 15 miles to the northeast, I have regarded the lower bed as 
 the Pittsburgh in constructing the above section. If, however, the coal 
 100 feet higher should prove to be the Pittsburgh, then 
 the 5-foot coal 150 feet above the bottom of the sec- 
 tion would probably be the Waynesburg bed, and the 
 Dunkard Greek series should be cut off just above it, 
 and thus shortened by 155 feet at this locality. 
 
 In the vicinity of Bellton, Marshall County, West 
 Virginia, 4 miles west from Board Tree Tunnel, the 
 exposures are very fine and the surface outcrops can 
 there also be combined with the record of an oil bor- 
 ing, which thus gives another measurement of the en- 
 tire series. 
 
 ' Section at Bellton , Marshall County , West Virginia . — 
 In descending from the highest summits near Bellton, 
 the following succession (Fig. 5) is obtained when 
 combined with an oil-boring record which was pub- 
 lished by the writer in the Annals of the Lyceum of 
 Natural History, New York, July, 1874 : 
 
 Bellton , Marshall County , West Virginia. 
 
 35' 
 
 
 
 
 
 284V immmm 
 
 
 ;cv.\v,v 
 
 
 [See map, Lj.] 
 
 Ft. Ft. in 
 
 1. Limestone, Windy Gap 5 1 
 
 2. Shales 30 
 
 3. 'Coal, Windy Gap, blossom 0 
 
 4. Concealed and sandstone and 
 
 shales 30 
 
 5. Shales and sandstone 60 
 
 6. Sandstone, massive, gray 20 } 333 
 
 7. Ked shales and concealed 75 
 
 8. Sandstone, massive 40 
 
 9. Red shales and sandstone. 50 
 
 10. Limestone 3 | 
 
 11. Shales and concealed 20 
 
 12. Coal, Nineveh 1 
 
 13. Shales and sandstone 35 
 
 14. Limestone and shales, Nineveh.. 10 
 
 15. Shales, sandstone and concealed. 100 
 
 16. Sandstone 5 
 
 17. Shales 10 
 
 18. Limestone 0 ( 
 
 19. Coal 0 ! 
 
 20. Shales and sandstone 15 
 
 21. Ked shales 5 284 8 
 
 •22. Concealed 20 
 
 23. Coal 1 
 
 24. Shales and concealed 30 
 
 25. Coal, Dunkard- ^^5 kslate 1 J'^ 1 3 
 
 26. Limy shales and fire clay 5 
 
 27. Shales 13 
 
 28. Limestone, gray, Jollytown 2 
 
 29. Shales and sandstones 30 
 
 30. Coal, Jollytown 0 8 J 
 
 31. Limestone, gray, Upper Wash- 
 
 ington (continued from oil- 
 well record) 5 ) 
 
 32. Sandstone 12 
 
 33. Shale - 7 
 
 34. Sandstone H 
 
 35. Shale 12 
 
 36. Fire clay 7 
 
 - 25 
 
 37. Sandstone 
 
 38. Shale 12 
 
 39. Sandstone 17 
 
 Fig. 5. — Section at Bellton, W. Va. 
 
WHITE.] 
 
 SECTION AT NEW MARTINSVILLE, W. VA. 
 
 2 7 
 
 Ft. in. 
 
 40. Coaly shales 9 
 
 41. Sandstone 9 
 
 42. Shale 5 
 
 43. Sandstone 4 
 
 44. Shale 19 
 
 45. Sandstone 16 
 
 46. Shale 4 
 
 47. Sandstone, 30 
 
 48. Shale 2 
 
 49. Sandstone 35 
 
 50. Shale 27 
 
 51. Sandstone 45 
 
 52. Coal, Washington 6 
 
 53. Sandstone 20 
 
 Ft. in. 
 
 313 
 
 Ft. in. 
 
 148 
 
 > 148 
 
 Ft. in. 
 
 54. Limestone 8 
 
 55. Shale 19 
 
 56. Sandstone 15 
 
 57. Shale 18 
 
 58. Sandstone 25 
 
 59. Shale 4 
 
 60. Limestone 10 
 
 61. Fire clay 3 
 
 62. Limestone 4 
 
 63. Sandstone 16 
 
 64. Place for Waynesburg 
 
 coal. 
 
 Total 1,078 8 
 
 This boring did not reach the Pittsburgh coal, and hence the identi- 
 fication of the 6-foot coal bed, 142 feet above the base of the section, is 
 made on the same basis as that of the 5-foot bed 150 
 feet above the bottom of Section 4, since the two coals 
 are evidently identical. The thin coals in the upper 
 half of the series have been named the Bellton group 
 from this locality. 
 
 Section at Neio Martinsville, West Virginia . — In pass- 
 ing south westward from this area of maximum devel- 
 opment of the Permo-Carboniferous rocks a considerable 
 change takes place in the character of the beds. The 
 Bellton coal group practically disappears, and also many 
 of the limestones, so that in the vicinity of New Martins- 
 ville, Wetzel County, West Virginia, the lower half of 
 the series presents the structure shown in Fig. 6 : 
 
 Net v Martinsville , Wetzel County, West Virginia. 
 
 |See map, M i.] 
 
 11 T* 
 
 Ft. 
 
 1. Red shale 
 
 2. Concealed 
 
 3. Red shale 
 
 4. Limestone, Nineveh, in several layers separated by shale 
 
 5. Red marly shale 
 
 6. Concealed and sandstone 
 
 7. Red shale 
 
 8. Sandstone, sandy shales, and concealed 
 
 9. Red shale 
 
 10. Sandstone, massive. 
 
 11. Concealed 
 
 12. Red shale 
 
 13. Concealed 
 
 14. Sandstone, brown massive 
 
 15. Sandy shales 
 
 16. Red shale _ 
 
 17. Sandstone 
 
 18. Red shale 
 
 19. Sandstone and sandy shales 
 
 20. Concealed and sandy shales 
 
 21. Red marly shales, with limestone nodules 
 
 22. Sandy shale, gray 
 
 23. Sandstone, massive - 
 
 24. Sandy shales 
 
 25. Red shale with limestone nodules 
 
 26. Shale, gray, sandy 
 
 27. Sandstone, massive 
 
 28. Sandy shales 
 
 29. Limestone, impure 
 
 30. Sandy shales 
 
 31. Coal, Washington 4 
 
 32. Sandy shales 5 
 
 33. Sandstone, massive 35 
 
 34. Concealed and sandy shales 25 
 
 35. Shales, sandstones, and concealed 50 
 
 36. Waynesburg coal. 
 
 Total 
 
 Ft. 
 
 5 
 
 45 
 
 2 
 
 10 
 
 5 
 
 30 
 
 5 
 
 30 
 
 10 
 
 10 
 
 35 
 
 5 
 
 25 
 
 10 
 
 23 
 
 2 
 
 25 
 
 5 
 
 25 
 
 20 
 
 5 
 
 15 
 
 20 
 
 15 
 
 5 
 
 2 
 
 30 
 
 3 
 
 2 
 
 20 
 
 119 
 
 563 
 
 Fio .6.— Section at New 
 Martinsville, W. Va. 
 
28 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 No. 4 appears to represent the Nineveh limestone, though its inter- 
 val above the base of the series is less here than usual. 
 
 Fig. 7. — Section at 
 .Baresville, Ohio. 
 
 Not a single one of the Beliton coals was observed in 
 this section, though some of them may have been pres- 
 ent and concealed. 
 
 (Section at Baresville , Ohio . — In the vicinity of Bares- 
 ville, Monroe County, Ohio, a long section was rnaile 
 by the late Prof. E. B. Andrews. It is referred to in 
 vol. II, Ohio Geology, page 587, and published on Map 
 XIII, section No. II. The locality is only 1 J miles above 
 New Martinsville, West Virginia, and the succession 
 reads as follows (Fig. 7) : 
 
 Baresville, Monroe County, Ohio . 
 
 [See map, M 1] 
 
 1. Coal, blossom 
 
 2. Concealed 
 
 3. Limestone, ineveli 
 
 4. Shale . . 
 
 5. Limestone, sandy 
 
 6. Red shale 
 
 7. Shale, mostly 
 
 8. Shale 
 
 y. Sandstone, laminated 
 
 10. Red shale 
 
 11. Sandstone 
 
 12. Red shale - ... 
 
 13. Sandstone 
 
 14. Shale 
 
 15. Sandstone 
 
 16. Red shale 
 
 17. Sandstone 
 
 18. Shale - 
 
 19. Sandstone 
 
 20. Shale 
 
 21. Coal, blossom, Jollytown 
 
 22. Shale 
 
 23. Sandstone 
 
 24. Sandy shale 
 
 25. Sandstone 
 
 26. Shale 
 
 27. Sandstone 
 
 28. Shale 
 
 29. Sandstone 
 
 30. Shale 
 
 31. Sandstone 
 
 32. Shale 
 
 33. Sandstone 
 
 34. Shale 
 
 35. Sandstone 
 
 36. Shale - 
 
 37. Sandstone 
 
 38. Shale - 
 
 ( Coal.... O' 9"1 
 
 39. Coal, Washington “A ’. < Clay . . . O' 4" S 
 
 t Coal.... 2' 0" > 
 
 40. Clay - 
 
 41. Shalle 
 
 42. Sandstone 
 
 43. Shale 
 
 44. Sandstone 
 
 45. Shale 
 
 46. Concealed 
 
 47. Sandstone, Waynesburg 
 
 48. Shale 
 
 49. Coal, Waynesburg. 
 
 Total 
 
 Ft. in. n 
 
 6 
 
 18 
 
 2 
 
 14 
 
 21 
 
 20 
 
 36 
 
 18 
 
 2 
 
 20 
 
 3 
 
 4 
 
 3 
 13 
 11 
 
 4 
 
 3 
 
 145 
 
 201 
 
 J 
 
 3 
 
 4 
 13 
 
 1 
 
 12 
 
 6 
 
 4 
 
 5 
 
 5 > 149 
 
 4 
 23 
 12 
 
 3 
 2 
 
 28 
 
 4 
 
 20 j 
 
 * 
 
 3 1 
 
 7 
 
 2 
 
 5 
 
 1 
 
 3 
 
 15,6 
 
 15 
 
 3 
 
 692 1 
 
WHITE. ] 
 
 SECTION AT WASHINGTON, PA. 
 
 29 
 
 The coal blossom at the summit of Section 7 appears to come at a 
 horizon above any of the Bellton beds, and hence is a new and prob- 
 ably extremely local element in the series. 
 
 Section in Liberty Toicnship , Washington County , 
 Ohio . — The following (Fig. 8) succession of the beds 
 in the lower portion of this series is reported by Mr. 
 F. W. Minshall from a hill near the Epler oil boring 
 in Liberty Township, Washington County, Ohio: 
 
 IQ 
 
 i40' 
 
 Liberty Township, Washington County, Ohio 
 
 [See map, M g.] 
 
 1. Shales and sandstones • 
 
 2. Coal, Jollytown 
 
 3. Shales and sandstone 1 
 
 4. Coal, Washington “A” 
 
 5. Shales and limestone 
 
 6. Sandstone 
 
 8. Ccal, Washington 
 
 9. Limestone and shales 
 
 12. Waynesburg coal. 
 Total 
 
 Ft. 
 
 Ft. 
 
 in. 
 
 
 100 
 
 
 
 1 
 
 8 
 
 
 140 
 
 
 
 2 
 
 6 
 
 31 ) 
 
 
 
 16 i 
 
 59 
 
 
 12 S 
 
 
 
 
 1 
 
 3 
 
 66 ) 
 
 
 
 28 > 
 
 100 
 
 
 6 J 
 
 
 
 
 404 
 
 5 
 
 59' 
 
 loo* 
 
 big ©. — Section ill 
 Washington County, 
 Ohio. 
 
 These identifications are made on the supposition 
 that the Macksburg coal of the Ohio geologists is the 
 equivalent of the Waynesburg bed. 
 
 Section at Washington , Pennsylvania. — In Washing- 
 ton County, Pennsylvania, the Dunkard series, as al 
 already stated, contains much more limestone than 
 elsewhere, and the intervals between 
 the several members are somewhat less 
 than in Greene County. The following 
 section (Fig. 9) from Geological Survey, 
 
 Pennsylvania, Report K, page 248, ex- 
 hibits the structure of the lower portion 
 
 of these beds at Washington, Pennsylvania : 
 
 Washington, Pennsylvania . 
 
 [See map. J 1.] 
 
 Ft. in. 
 
 Limestone, Jollytown 
 
 Shale 
 
 Coal, Jollytown 
 
 Sandstone 10 
 
 Dark shale 8 
 
 Limestone, Upper Washington 30 
 
 Concealed 50 
 
 Coal, blossom 0 
 
 Concealed 80 
 
 Limestone, Lower Washington 12 
 
 Coal, Washington 7 
 
 Clay 4 
 
 Sandstone 9 
 
 Concealed 10 
 
 Limestone. 2 
 
 Shales, limestone, and concealed 65 
 
 Black slate 3 
 
 Limestone 4 
 
 Blue shale 15 
 
 Waynesburg coal. 
 
 Total 
 
 Ft. 
 
 10 
 
 190 
 
 S 117 0 
 
 323 6 
 
 Pig. 9. — Section at 
 
 Waelmigtou, Ta, 
 
30 THE NORTHERN BITUMINOUS COAL FIELD. [bull. 65. 
 
 Section near Taylorstown , Pennsylvania . — Another section, from the 
 same volume page 259, exhibits the succession in the lower half of this 
 series in Buffalo Township, Washington County, Pennsylvania, as 
 shown in Fig. 10. 
 
 In both these sections (9 and 10) the writer has changed the identi- 
 fications of some of the beds (notably that of the Jollytown coal) from 
 that made in the original sections by Stevenson, but in every such case 
 the change is clearly warranted, since the coal in question was placed 
 too near the Washington coal by Stevenson. 
 
 Near Taylorstown , Washington County , Pennsylvania. 
 
 [See map, J k.] 
 
 Ft. in. 
 
 1. Limestone, in fragments 
 
 2. Shales and sandstone 
 
 3. Coal, blossom, Jollytown 0 
 
 4. Shale 10 
 
 5. Limestone 6 
 
 6. Concealed 20 
 
 7. Limestone 12 
 
 8. Sandstone .. 15 
 
 9. Coal .* 0 8 
 
 10. Concealed 40 
 
 11. Limestone 15 
 
 12. Concealed 45 
 
 13. Limestone 10 
 
 14. Concealed 5 
 
 15. Coal 0 
 
 16. Concealed, with much limestone 25 
 
 17. Coal, Washington 6 
 
 18. Concealed, with a limestone 85 
 
 19. Coal, blossom, Waynesburg “B ” : 0 
 
 20. Concealed 40 
 
 21. Coal, blossom, Waynesburg “A” . 0 
 
 22. Waynesburg sandstone 50 
 
 23. Shales 10 
 
 24. Coal, Waynesburg 
 
 Total 
 
 Ft. in. 
 
 0 
 
 40 
 
 1 
 
 > 203 8 
 
 J 
 
 1 
 
 I 
 
 0 
 
 384 8 
 
 The very highest beds of the Dunkard Creek series known to the 
 writer occur in Shougli’s Knob, at the head of Dunkard Creek, Gilmore 
 Township, Greene County, Pennsylvania, but these are concealed by a 
 thick covering of soil, and hence could not be seen in detail. The high- 
 est rock of the series which has been traced over any considerable area 
 is the Windy Gap Limestone. 
 
 CHARACTERISTIC HORIZONS. 
 
 TIIE WINDY GAF LIMESTONE. 
 
 This has been named from its occurrence near Windy Gap, a “ divide ” 
 separating the Laurel llun branch of Fish Creek from the waters of 
 Wheeling Creek, in Springhill Township, Greene County, Pennsylvania, 
 
WHITE.] 
 
 CHARACTERISTIC HORIZONS. 
 
 31 
 
 The stratum is usually of a bluish gray color, quite pure, and has a 
 thickness of about five feet. It contains minute fresh water fossils, 
 and occasionally small crystals of blende. 
 
 The only land geologically and topographically high enough to catch 
 this stratum is that which clusters about the southwestern corner of 
 Pennsylvania, in Greene County, and the adjoining regions of Mar- 
 shall, Wetzel, and Monongalia, in West Virginia. Only one point 
 (Hunsucker’s Knob) in the last county is high enough to catch this 
 limestone, since its outcrop ranges between 1,500 and 1,600 feet above 
 the sea. The sections (Figs. 3 and 4) at Board Tree and Bellton, in 
 Marshall County, as well as the one (Fig. 2) in Aleppo Township, 
 Greene County, show this stratum near their summits, but its horizon 
 is concealed in Shough’s Knob of the Dunkard Creek section (Fig. 1). 
 
 This is the same stratum as that numbered Limestone XIV by Prof. 
 John J. Stevenson in his Eeport K, Second Geological Survey of Penn- 
 sylvania. 
 
 THE WINDY GAP COAL. 
 
 At an interval of 25 to 30 feet below the limestone just described 
 there occurs a small coal bed just under the summit of the “ divide” at 
 Windy Gap, Greeue County, Pennsylvania, and it has been designated 
 from that locality. Xo opening into it has ever been made, and hence 
 it is known only as a blossom which exposes one to two feet of coal and 
 black slate, the latter filled with the fossil Cypris, or a closely allied 
 form. 
 
 The same bed was also seen in Aleppo Township, and in the summit 
 of the hills at Bellton. It is the highest known coal of the series, and 
 comes about 1,050 feet above the Waynesburg bed. 
 
 * THE GILMORE SANDSTONE. 
 
 Crowning the upper portion of the Permo-Carboniferous beds over a 
 considerable area around the heads of Dunkard, Wheeling, and Fish 
 Creeks, there occurs a very massive sandstone having a thickness of 25 
 to 40 feet. It was named the Gilmore sandstone by Professor Steven- 
 son, from its occurrence in the township of that name in southwestern 
 Greene County. This stratum is usually a coarse and very massive 
 sandstone, excellent for building purposes, and often forming long lines 
 of cliffs on the summits of the high ridges. These cliffs are always 
 traversed with fissures, and they furnish a convenient retreat for foxes 
 when chased by hounds, so that the stratum in question is often locally 
 known as the u Fox rocks,” and again it is named from the farms where 
 the cliffs occur, as “Pethtle” rocks, “ Efaw” rocks, etc. This stratum 
 has been the main agency in preserving all of the very high beds of 
 the Permo-Carboniferous from erosion. 
 
 The interval below the Gilmore sandstone for 200 to 250 feet consists 
 of red shales, occasional thin limestones, and gray sandstones, but con- 
 
32 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65 . 
 
 tains no beds sufficiently characterized to be identifiable over any con- 
 siderable area. 
 
 THE NINEVEH SANDSTONE. 
 
 At 225 to 250 feet below the Gilmore sandstone, we come to another 
 great sandstone deposit which, from its good development near the vil- 
 lage of Nineveh, Greene County, Pennsylvania, has been designated 
 from that locality. Like the Gilmore sandstone above, it is usually 
 an excellent building stone, and has long been used for that purpose 
 on the Baltimore and Ohio .Railroad, near Littleton, Wetzel County, 
 West Virginia, where it crops out in a great cliff along the hills 150 to 
 200 feet above creek level. 
 
 This same stratum may also be seen in the hills two miles above Jol- 
 lytown, Greene County, where it has long been quarried on the land 
 of Thomas White for building purposes. It is of a yellowish gray cast, 
 rather coarse-grained, but soft, and splits readily into rectangular 
 blocks. 
 
 THE BELLTON COAL GROUP. 
 
 At 275 to 300 feet under the Gilmore sandstone we find the upper- 
 most of a series of thin coals which, from their fine exposure at the vil- 
 lage of Bellton, Marshall County, West Virginia, have been termed the 
 Bellton group. These coate, few of which are rarely more than one 
 foot thick, occur within a rock interval of 200 to 300 feet, and when all 
 are present, as in the Bellton section (Fig. 5), there are five distinct beds, 
 though not all of them are persistent over auy considerable area. The 
 three beds given in the Dunkard Creek section (Fig. 1), viz, the Nine- 
 veh, Dunkard, and Jolly town coals, are the most important members 
 of the group. Interstratified with these coals are shales^ sandstones, 
 and two important limestones. 
 
 THE NINEVEH COAL. 
 
 This is the uppermost member of the Bellton group, and was named 
 from the village of Nineveh, Greene County, Pennsylvania, by Professor 
 Stevenson. 
 
 The coal rarely exceeds one foot in thickness, yet it is generally quite 
 pure, and is frequently used for smithing purposes. 
 
 In the hills at Bellton it crops out 290 feet above Fish Creek, and the 
 same coal is seen in the railroad cut at the western portal of Board 
 Tree Tunnel, 75 feet above track level. 
 
 On the head waters of Dunkard Creek it is known as the John Tay- 
 lor coal, and although only one foot thick is highly valued as a smithing 
 fuel. 
 
 THE NINEVEH LIMESTONE. 
 
 Below the Nineveh coal at an interval of 25 to 30 feet there comes a 
 limestone which has a very extended distribution. It was called Lime- 
 stone No, X by Professor Stevenson in his .Report K, Greene and Wash- 
 
WHITE.] 
 
 CHARACTERISTIC HORIZONS. 
 
 33 
 
 ington Counties, but itis here designated from the same village in Greene 
 County which has given name to the coal and sandstone already de- 
 scribed. 
 
 This limestoue usually consists of several layers separated by shales 
 the whole of which sometimes foots up nearly 20 feet, as in the section 
 at Board Tree Tunnel (Fig. 4), but its usual thickness is seldom more 
 than 10 feet. Frequently a stratum of bituminous shale is found inter- 
 stratified with the layers of limestone. Some of the latter are quite 
 pure, and furnish excellent lime. It has a very wide distribution, as 
 may be seen from its presence in each of the first seven sections already 
 given. The same stratum extends clear through to Jackson County, 
 West Virginia, and nearly to the Big Kanawha Biver, where it occurs 
 high up on the summits of the hills and is hence termed the “ Ridge v 
 limestone, by the farmers. 
 
 There is a fine exposure of this rock at Limestone Hill Post-office, on 
 the Parkersburg and Charleston turnpike, near the corners of Wirt, 
 Wood, and Jackson Counties, West Virginia. It is there nearly 30 feet 
 thick, in several layers, and contains many minute fossils, all apparently 
 of fresh- water types. 
 
 THE HOSTETTER COAL. 
 
 Occasionally a bed of coal occurs at 75 to 100 feet below the Nineveh 
 limestone. It has been stripped out of the run on the old Hostetter 
 farm near Burton, Wetzel County, West Virginia, where it is 12 to 15 
 inches thick and rather pure. It also appears to be present in some 
 localities near the head of Dunkard Creek, and in a local section near 
 Bellton it was seen 15 inches thick at 130 feet below the Nineveh coal. 
 
 THE FISH CREEK SANDSTONE. 
 
 At 135 to 150 feet below the Nineveh coal, there often occurs a very 
 massive sandstone. It makes the great cliffs along the waters of Fish 
 Creek in Springhill Township, Greene County, Pennsylvania, and was 
 designated from this stream by Stevenson in his Report K. 
 
 The rock in question is frequently quite massive, and it makes an ex- 
 cellent building stone. It is very conspicuous in the region of Deep 
 Valley, Pennsylvania, where it forms long lines of vertical cliffs 25 to 
 30 feet high. It may also be seen in cliffs along the Baltimore and Ohio 
 Railroad, above Littleton, in Wetzel County, where it is quarried for 
 building purposes. 
 
 THE DUNKARD COAL. 
 
 Below the Fish Creek sandstone, at an interval of 1 to 20 feet, another 
 coal bed is often found, which, from its occurrence along the bed of 
 Dunkard Creek for a considerable distance, was named the Dunkard coal 
 by Professor Stevenson. It is seldom more than 12 to 15 inches thick, 
 but is almost invariably double, having a thin layer of slate near its 
 Bulk 05 3 
 
34 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 ^BULL. 65. 
 
 center. At Deep Valley, Pennsylvania, however, this parting thick- 
 ens up to five feet or more aiul thus separates the coal into two well- 
 defined beds, each of which is 8 to 10 inches thick. In the roof shales 
 of this coal at Mr. Lee Garrison’s, in Gilmore Township, Greene County, 
 Pennsylvania, finely preserved fossil plauts abound, principally of the 
 genera Neuropteris and Odontopteris. 
 
 This bed is frequently stripped along the streams for local use in 
 Greene, Monongalia, Wetzel, and Marshall Counties. 
 
 THE JOLLYTOWN LIMESTONE. 
 
 Below the Dunkard coal, at an interval of 25 to 30 feet, there occurs 
 a bed of limestone which is rather persistent. It is well exposed in the 
 vicinity of Jollytown, Greene County, Pennsylvania, and has been des- 
 ignated from that locality. As may be seen from its presence in Sec- 
 tions 1 to 5 and also in 9, this limestone has a wide distribution, though 
 at the head of Dunkard (Fig. 1), and on Fish Creek (Fig. 5), the stratum 
 is only 1 to 2 feet thick. In Washington County, Pennsylvania, how- 
 ever, it thickens up to 10 feet or more and is usually a rather pure lime- 
 stone. 
 
 THE JOLLYTOWN COAL. 
 
 This is the lowest member of the Bellton coal group, and underlies 
 the Jollytown limestone by an interval of 25 to 30 feet. The coal was 
 named by Professor Stevenson from a village in Greene County, Penn- 
 sylvania. 
 
 This is the only coal of the Bellton group that ever attains dimen- 
 sions of 2 to 3 feet, and can therefore be mined by drifting, since in 
 the vicinity of Wise, Monongalia County, West Virginia, and below 
 this along the South Fork of Dunkard Creek, it is nearly 3 feet thick, 
 and is mined to a considerable extent for local use. The coal is not 
 very pure, but in the absence of any other beds it finds a ready market. 
 In the Bellton section (Fig. 5) this coal has been identified with the 
 lowest bed exposed there. This is only a few inches thick and quite 
 slaty, so that it is possible the Jollytown bed is the one next above, and 
 which in that section has been referred to the Dunkard coal. 
 
 Along Dunkard Creek the Jollytown coal is nearly always present, 
 and seldom less than 1 to 2 feet thick. It becomes a very important 
 key rock over a wide region, since there are seldom any other coals 
 below it for an interval of 250 feet. It extends almost without a break 
 across Greene, Monongalia, Marion, and Harrison Counties, but appears 
 to thin away in Doddridge. 
 
 Throughout Monongalia, Greene, and Marshall Counties, the interval 
 between this bed and the Washington coal below is about 275 feet, 
 but westward, in Washington County, Ohio (Section 8), the interval 
 thins away to 200 feet, and practically the same measurement is found 
 in Washington County, Pennsylvania (Sections 9 and 10). 
 
WHITE.] 
 
 CHARACTERISTIC HORIZONS. 
 
 35 
 
 THE UPPER WASHINGTON LIMESTONE. 
 
 Three limestones were named from Washington, Pennsylvania, by 
 Professor Stevenson — an Upper, Middle, and Lower one — and two of 
 these are shown in the section (Fig. 9) from the typical locality. 
 
 The Upper Limestone is a very important bed in Washington County, 
 since it has a thickness of 20 to 30 feet, and is generally very pure. It 
 is usually of a dark blue color, and is much used for macadamizing 
 roads and burning for agricultural and other purposes. This rock ap- 
 pears to be identical with the limestone seen in the bed of Dunkard 
 Creek near the mouth of Negro Bun, above Jolly town, Greene County, 
 Pennsylvania, where it carries a bituminous shale on its top, filled with 
 fish remains and other minute fossils, and underlies the Jollytown coal. 
 
 In the bed of Fish Creek at Bellton, Marshall County, TVest Virginia, 
 we find a limestone with a fish bed on its top, which appears to be iden- 
 tical with the Upper Washington deposit. 
 
 THE MIDDLE WASHINGTON LIMESTONE. 
 
 About midway in the interval between the Upper Washington lime- 
 stone and the Washington coal there is frequently found another lime- 
 stone bed. It is very persistent in Washington County, Pennsylvania, 
 and is often 15 to 20 feet thick and of a huffish color. 
 
 On Dunkard Creek it appears to be represented by a stratum seen 
 just above the road at Kent’s Mills, where it is only three feet thick. 
 This limestone, like all of those in the Dunkard series, contains minute, 
 undetermined fossils, and the bituminous shales accompanying them 
 hold plenty of fish scales, teeth, etc., as well as fragments of plants. 
 
 WASHINGTON “a” COAL. 
 
 At 70 to 80 feet above the Washington coal, there occurs a bed of 
 impure coal and coaly shale- which is often present in the section along 
 Dunkard Creek. Sometimes the ehtire bed is four to five feet thick, 
 but little of it is ever merchantable coal, being seldom more than a 
 bituminous slate. It is well exposed in the hills about Blacksville, 
 and Brownsville, in Monongalia County, and there contains many bi- 
 valve crustaceans. 
 
 Bituminous shale is often found at this horizon in Washington and 
 Greene Counties, Pennsylvania, and in Washington County, Ohio (Fig. 
 8), a coal bed 2J feet thick seems to occur at the same place in the series. 
 
 THE MARIETTA SANDSTONES. 
 
 The Washington “A” coal is often absent, and the portion of the 
 series for 100 to 125 feet above the Washington coal is then frequently 
 occupied by two or three beds of massive sandstone. These crop out 
 in the hills below Marietta, Ohio, where they have long been exten- 
 sively quarried for grindstones and building stone, and they have been 
 
36 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65. 
 
 designated from that locality. There are often three of them, each 25 
 to 40 feet in thickness, and separated by thin shales, so that in such 
 cases they might be called the Upper, Middle, and Lower Marietta 
 sandstones. Sometimes, however, as near Bock Lick, Marshall County, 
 West Virginia, the shales thin out and let all of the sandstones coalesce 
 into one mass more than 100 feet thick. 
 
 These beds form the great cliffs at Eaven Eock, Pleasants County, 
 West Virginia. The upper one is extensively quarried at the Jackson 
 quarry in Parkersburg, West Virginia, and it with its associated rocks 
 forms long lines of cliffs up the Little Kanawha Eiver, where they have 
 been extensively quarried in the vicinity of Elizabeth and other points. 
 
 It is one of these beds that makes the big cliffs on the hill above the 
 famous McGugan gas well in Washington County, Pennsylvania. 
 These rocks are sometimes gray, but more frequently of a yellowish or 
 huffish cast, and moderately coarse in grain. They also occur in Bitch ie ? 
 Wirt, Jackson, and Putnam Counties, West Virginia, where they cap 
 the narrow ridges in long lines of cliffs. 
 
 In Greene and Washington Counties, Pennsylvania, and Monongalia 
 County, West Virginia, this interval of 100 feet above the Washington 
 coal is generally occupied by shales, limestones, and thin, sandy beds, 
 massive sandstones being exceptional. 
 
 THE BLACKSVILLE LIMESTONE. 
 
 In some portions of Washington, Greene, and Monongalia Counties, 
 a limestone occurs with considerable persistency at 30 to 50 feet above 
 the Washington coal. This was numbered Limestone III by Professor 
 Stevenson in his Greene and Washington report, but as it comes to the 
 surface near the bed of Dunkard Creek, in the village of Blacksville, 
 Monongalia County, West Virginia, it has been given a geographical 
 name from that locality. The rock is generally gray, quite pure, and 
 only three to five feet thick. It is seen in Section 2 at 46 feet above 
 the Washington coal. It soon disappears southward from the Pennsyl- 
 vania line. 
 
 THE LOWER WASHINGTON LIMESTONE. 
 
 At Washington, Pennsylvania, a limestone of unusual thickness (20 
 feet) forms the roof of the Washington coal, and it was designated, from 
 that locality, the Lower Washington limestone by Stevenson. It has 
 a wide distribution in Greene, Washington, Ohio, Belmont, Marshall, 
 and Monongalia Counties, but disappears southward from these. It 
 often attains a thickness of 20 to 30 feet in Washington County, but is 
 always interstratified with much shale, and outside of Washington 
 County is seldom more than 5 to 10 feet thick. Frequently some of the 
 layers contain so much carbonate of iron as to prove a fair ore. These 
 iron-bearing layers are often interstratified with bituminous shales, and 
 in such cases tbe iron layers are covered with fossil plants. It is on 
 
WHITE.] 
 
 CHARACTERISTIC HORIZONS. 
 
 37 
 
 these thin, shaly layers of carbonate of iron in the roof of the Washing- 
 ton coal at Brown’s Bridge, Dunkard Creek, on the West Virginia- 
 Pennsyl vania line, that the Permian plant, Callipteris conferta , occurs 
 as described in Report PP, Second Geological Survey, Pennsylvania, 
 page 54. 
 
 THE WASHINGTON COAL. 
 
 This bed, which is the only one in the Dunkard series that is worka- 
 ble over a wide area, was first described by the writer, and named the 
 Brownsville coal from its occurrence at the village of that name in 
 Monongalia County, West Virginia. Subsequently, however, the same 
 coal was found in greater development at Washington, Pennsylvania, 
 and it was designated from that locality by Professor Stevenson. 
 
 It is always a multiple bed, being separated into two or three layers 
 by divisions of slate. Occasionally these divisions are numerous and 
 the entire thickness of the bed is 8 to 10 feet, -but in all cases the only 
 pure or merchantable coal is the bottom portion, which seldom exceeds 
 two and a half to three feet. The upper part of the bed is nearly 
 always very impure, since it contains so much ash and slate as to consti- 
 tute it a mere bed of richly bituminous shale. 
 
 This coal is much more persistent than any other coal of the Permo- 
 Carboniferous series, since it occurs everywhere in the northern area of 
 these rocks, and does not disappear to the southwest except beyond the 
 Little Kanawha River, in West Virginia, while in Ohio it seems to be 
 persistent even to the southwestern margin of these deposits. In Wash- 
 ington and Meigs Counties, Ohio, it is frequently referred to by Pro- 
 fessor Andrews as the Hobson coal. 
 
 (Section at Farmington , Marion County , West Virginia . — The following 
 section of this coal, taken near Farmington, Marion County, West Vir- 
 ginia, well illustrates the structure of the bed when it is thick : 
 
 1. 
 
 2 . 
 
 3 . 
 
 4 . 
 
 5 . 
 
 6 . 
 
 7 , 
 
 8 . 
 
 9 . 
 
 10 . 
 
 11 . 
 
 12 . 
 
 13 . 
 
 14 . 
 
 Coal 
 
 Shale 
 
 Coal and shale 
 
 Coal 
 
 Shale 
 
 Coal 
 
 Shale 
 
 Coal 
 
 Shale 
 
 Coal 
 
 Shale 
 
 Coal, fair 
 
 Slate 
 
 Coal, good 
 
 Ft. in. 
 . 0 6 
 . 0 3 
 . 0 8 
 . 1 0 
 . 0 4 
 . 0 5 
 . 0 3 
 . 1 0 
 . 0 4 
 . 1 1 
 . 0 3 
 . 2 0 
 . 0 2 
 . 2 6 
 
 1 
 
 4 
 
 in. 
 
 n 
 
 Ft. in. 
 >10 9 
 
 8 
 
 Here the upper or roof portion of the coal, although 0 feet thick, is 
 entirely worthless, and the only really good coal in the bed is the 2£ 
 feet at the bottom. 
 
38 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65. 
 
 Through Washington County, Pennsylvania, this coal has a thick- 
 ness of 5 to 6 feet, but very little of it is merchantable. 
 
 It is frequently exposed along the Ohio River hills between Wheel- 
 ing and Parkersburg, being at low water in the latter town. 
 
 Before disappearing to the southwest it dwindles down in thickness 
 very much, since at Harrisville, Ritchie County, it is only 2 feet 
 thick, and at the Grahamite mines, near Hughes River in the same 
 county, only feet. 
 
 It is mined for local supply in the vicinity of Smith ville, Ritchie 
 County, where it is only 15 inches thick and 150 feet above the level 
 of Hughes River. 
 
 Section on Willey Fork, Wetzel County, West Virginia. — At the mouth 
 of the Willey Fork of Fishing Creek, Wetzel County, West Virginia, 
 this coal is brought a few feet above water level by a low, anticlinal roll, 
 and there it exhibits the following structure : 
 
 1. Dark shales 
 
 2. Coal 
 
 3. Coaly shale 
 
 4. Shale, gray, sandy 
 
 5. Coal 
 
 6. Gray shales *, 
 
 7. Coal, slaty 
 
 Ft. 
 
 in. 
 
 0 
 
 5 " 
 
 1 
 
 6 
 
 2 
 
 0 
 
 0 
 
 3 
 
 . 2 
 
 0 
 
 2 
 
 0 j 
 
 Section near Brown’s Mills , Monongalia County , West Virginia. — Rear 
 Brown’s Mills, Monongalia County, where this coal was first described, 
 it has the following structure: 
 
 Ft. in. 
 
 1. Bituminous shale 
 
 2. Coal, impure 
 
 3. Shale 
 
 4. Coal, slaty 
 
 5. Shale 
 
 6. Coal, good 
 
 2 0 
 
 1 4 
 0 3 
 
 2 4 > 
 
 Ft. 
 
 8 
 
 At this locality the Lower Washington limestone forms the roof 
 above the bituminous shale Ro. 1, and it also contains much iron. 
 
 Occasionally a thin coal is found resting immediately on top of the 
 Lower Washington limestone, and that condition of affairs exists at 
 Brown’s Mills, where a bed of coal and black slate, in all 2 feet thick, 
 occurs 10 feet above the top of the Washington coal. The bed is not 
 persistent enough to merit a separate name, however. 
 
 THE WASHINGTON SANDSTONE. 
 
 Very frequently no fire clay is present under the Washington coal, 
 and the latter rests directly upon a flaggy sandstone, often finely 
 laminated, brown, micaceous, and containing vegetable fragments in 
 great quantity. This stratum, which was called the Washington sand- 
 
WHITE. ] 
 
 CHARACTERISTIC HORIZONS. 
 
 39 
 
 stone by Professor Stevenson, occurs over a wide area in Monongalia, 
 Greene, and Washington Counties, but is not persistent very far south 
 of the Pennsylvania line. 
 
 THE LITTLE WASHINGTON COAL. 
 
 Just under the Washington sandstone, and 10 to 20 feet below the 
 Washington coal, there sometimes occurs a thin bed of coal, seldom at- 
 taining afoot in thickness. It is more persistent in Washington County, 
 Pennsylvania, than elsewhere, and hence was designated as above by 
 Stevenson. It is seldom seen south from the Pennsylvania line, and in 
 Greene County even is represented only by a thin bed of bituminous 
 slate. 
 
 THE WAYNESBURG “b” COAL. 
 
 Below the last little coal bed there usually occur shales, thin sand- 
 stones, and occasionally a limestone, down to about 45 feet below the 
 Washington coal, where another small bed is found quite persistent in 
 Monongalia, Greene, and Washington Counties. It is seldom more than 
 a foot thick, but sometimes attains to two. It has never been seen south 
 of Monongalia County, and is of little economic importance. 
 
 THE COLVIN , S RUN LIMESTONE. 
 
 Below the last coal come 30 to 35 feet of shale and thin sandstones, 
 and then we get a limestone that was numbered Limestone 1(a) by 
 Professor Stevenson, but I have given it the above geographical desig- 
 nation from its occurrence at the locality of Section 2, where it is 3 
 feet thick and quite pure. It is often of a bullish cast, however, and 
 contains too much iron to slake well on burning. In Washington 
 County, Pennsylvania, this stratum thickens up to 8 and 10 feet, but it 
 is seldom seen south of the Pennsylvania line. 
 
 THE WAYNESBURG “a” COAL. 
 
 This occurs just under the last mentioned limestone and like it is con- 
 fined to the northern end of the Permo-Carboniferous area. It some- 
 times attains a thickness of 3 and 4 feet, but is generally slaty and 
 worthless, so that it has seldom been mined. It occurs quite generally 
 across Monongalia, Marion, and Harrison Counties, and is possibly 
 present in Ritchie County near Harrison ville, but beyond that it has not 
 been identified. Its horizon is usually GO to 80 feet above the Waynes- 
 burg coal proper. 
 
 THE MOUNT MORRIS LIMESTONE. 
 
 Separated from the coal last described by only 2 to 5 feet of clayey 
 shales there sometimes occurs a limestone which, although noted, 
 was not named by Stevenson in his Report K. It is well exposed on 
 the north bank of Dunkard Creek at Mount Morris, Greene County, 
 Pennsylvania, and has been designated from that locality. The stratum 
 
40 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65 . 
 
 is often only 1 to 2 feet thick, and seldom more than 5 feet except 
 in Washington County, Pennsylvania, where it is occasionally thicker. 
 
 This limestone is not persistent, and is seldom found south of the 
 Pennsylvania line, being frequently absent even in Greene and Wash- 
 ington Counties. 
 
 THE ,WAYNESBURG SANDSTONE. 
 
 Just under the horizon of the Mount Morris limestone, and separated 
 from it by 2 to 5 feet of shales and clay, there comes a very im- 
 portant sandstone. This was long ago termed the Waynesburg sand- 
 stone, from its fine development near the town of that name in Greene 
 County, Pennsylvania. It is one of the most persistent members of the 
 Permo-Carboniferous series, since its eastern outcrop can be followed 
 in an almost constant line of cliffs from Greene County, Pennsylvania, 
 clear across West Virginia to the Big Kanawha River at Winfield. 
 
 This stratum is the only one in the series that is generally con- 
 glomeratic or contains quartz pebbles larger than coarse sand grains. 
 On account of this peculiarity the rock in question becomes a very im- 
 portant guide to the geologist in the interior of West Virginia, where 
 so many of the Dunkard Creek coals and limestones have disappeared, 
 for it retains its pebbly character over a very wide area. When at its 
 greatest development the thickness of this stratum approaches 75 and 
 even 100 feet. It is usually a grayish white rock, with a yellowish 
 cast on freshly broken surfaces, and its weathered bowlders are usually 
 covered with ridges and streaks of harder iron -bearing sand. The rock 
 splits readily and frequently furnishes excellent building stone, the 
 piers of the Baltimore and Ohio Railroad bridges across the Monongahela 
 River near Fairmont having been constructed of it. 
 
 Along the western border of the outcrop of this rock it dwindles 
 down and changes its character entirely, being frequently represented 
 in Washington County, Pennsylvania; Marshall and Ohio Counties, 
 West Virginia ; Belmont and Monroe Counties, of Ohio, by sandy shales 
 and flaggy sandstones, and occasionally even a stratum of limestone 
 may be found at this horizon. 
 
 In passing down the Ohio River below Marshall County the horizon 
 of this sandstone passes below water level, but when it reappears near 
 Saint Mary’s, in P leasants County, the rock has regained its massive- 
 ness, and is a coarse pebbly sandstone 50 feet thick, and from this 
 point on down the Ohio River, whenever above the level of the same, 
 it is always a massive sandstone. From Blennerhasset Island, below 
 Parkersburg, this rock is almost constantly visible either in the bed 
 or bluffs of the Ohio on down to 25 miles below the mouth of the 
 Great Kanawha. It is the emergence of this stratum from the bed of 
 the stream which makes Letart Falls in the Ohio River. It is this rock 
 which forms the great cliffs in the top of the hills at Red Rock, in Put- 
 
WHITE.] 
 
 AGE OP THE DUNKARD CREEK SERIES. 
 
 41 
 
 narn County, on the Great Kanawha, and the same may be seen as a 
 bed of pebbly sandstone at many points in Ritchie, one at the famous 
 Grahamite mine being especially noteworthy, for it is the great sand- 
 rock through which the celebrated fissure extends at the base of the 
 hills, and it is there 75 feet thick. 
 
 Through Ritchie, Gilmer, and Calhoun Counties a bed of brecciated 
 limestone occurs at the base of this stratum and incorporated with it, 
 which is quite persistent and seems to replace the usual underlying 
 Wavnesburg coal, which is there absent. 
 
 THE CASSVILLE PLANT SHALE. 
 
 The Waynesburg sandstone often rests directly on the underlying 
 Waynesburg coal, but more frequently a bed of dark gray shale, 5 to 
 15 feet thick, intervenes. This shale is always prolific in fossil plants and 
 is especially so in the vicinity of Cassville, Monongalia County, West 
 Virginia. It is from this locality and horizon that so many of the fos- 
 sil plants were obtained which are described in the Second Geological 
 Survey, Pennsylvania, Report PP, by Fontaine and White, and it is 
 from the same shale that so many plants of Permian and even Triassic 
 types have been procured, Tseniopteris, Saportma, Baiera, and Pa- 
 chypteris being among the number. No systematic search has ever 
 been made at any other locality, and hence it is entirely probable that 
 the list of fossil plants could be largely increased were this bed thor- 
 oughly explored in other regions. Other promising localities of the 
 Cassville shale which have been slightly explored are CarmichaePs, 
 Greene County, Pennsylvania; Georgetown, Monongalia County ; and 
 West Union, Doddridge County. In connection with these roof shales, 
 and sometimes interstratified with the top members of the underlying 
 coal, there occur at Cassville numerous remains of insects, the princi- 
 pal ones being fossil cockroaches, of which Gerablattina seems to be 
 the principal genus. 
 
 THE AGE OF THE DUNKARD CREEK BEDS. 
 
 The fauna of these rocks has never been systematically studied and 
 its relationships determined. What desultory work has been done in 
 this line goes to show that the animal forms consist principally of mi- 
 nute shells of crustaceans, fish remains, and insects, many of which are 
 probably undescribed. No Brachiopods have ever been seen in these 
 rocks, and hence one important line of evidence which might help to 
 determine their relative age is wanting. Some geologists have been 
 inclined to regard them as belonging in the Carboniferous proper be- 
 cause of the absence of the Permian reptilian fauna, and other types 
 common elsewhere, but as the deposits are mainly of fresh water origin, 
 the absence of such types is to be expected. Hence until the minute 
 fauna occurring in these limestones and black slates shall have been 
 carefully studied, the geologist must rely on the evidence of fossil plants. 
 
42 THE NORTHERN BITUMINOUS COAL FIELD [bull. 65 . 
 
 These have been studied by Prof. Wm. M. Fontaine and the writer, 
 the results being published in Report TP, Second Geological Survey, 
 Pennsylvania. The conclusions there given show that the flora is 
 closely ana unmistakably allied to the Permian of Europe, since it con- 
 tains so many types that are peculiar to those rocks or even related to 
 Mesozoic forms. The facts and conclusions set forth are sufficient to 
 convince Prof. Archibald Geikie that these rocks are of the same age 
 as the reptiliferous beds at Autun. 
 
 The conclusion that these rocks are of Permian age has not been ac- 
 cepted by all American geologists, though none have given any reasons 
 for discrediting the evidence of the fossil plants on which it is based, 
 and until it is contradicted by the animal remains or otherwise shown 
 to be erroneous, no other hypothesis is tenable in view of the evidence 
 at hand. The list of plants from which the Permian age of these Dunk- 
 ard beds is inferred, together with the general discussion of the same, 
 is given m Chapter III, pages 105, 120, Report PP, Second Geological 
 Survey, Pennsylvania. 
 
 The recent discovery of an undoubted Permian invertebrate fauna in 
 Texas by Prof. C. A. White and Mr. Cummins (American Naturalist, 
 February, 1889), confirms the conclusions of Profs. Cope and Marcou 
 with reference to the existence of a great Permian series of rocks in 
 this country, and hence there is no longer any reason for doubting that 
 America contains deposits which are equivalent in part at least to the 
 Permian of Europe. The Texas deposits, as described by Prof. White 
 in the article referred to, are so exactly similar lithologically to these 
 uppermost beds of the Appalachian region, that the description of the 
 one might well answer for that of the other, and there can be very little 
 doubt that the two series are equivalent. Singularly enough the beds 
 have practically the same thickness, 1,000 feet in Texas, and 1,100 in 
 West Virginia and southwest Pennsylvania. 
 
CHAPTER III. 
 
 THE UPPER COAL MEASURES, OR MONONGAHELA RIVER SERIES. 
 
 THICKNESS, CHARACTER, AND EXTENT. 
 
 This series of rocks begins at base with the Pittsburgh coal and 
 extends up to the Cassville shale. The thickness varies between 200 
 feet along the northwestern outcrop in Ohio and 380 feet in the Monon- 
 gahela River region, but in the center of the Appalachian trough a 
 boring at Browntown, Harrison County, West Virginia, carefully meas- 
 ured with steel line, reveals a thickness of 413 feet from the top of the 
 Waynesburg coal to the bottom of the Pittsburgh bed. 
 
 Within the interval there belong six distinct coal beds, though only 
 four of these are workable over any considerable area. These coals 
 have their greatest development along the waters of the Monongahela 
 River, and hence the series was long ago named after that river by 
 Prof. H. D. Rogers. 
 
 The character of the rocks interstratified with the coal beds changes 
 greatly in passing from the Monongahela River southward to the Great 
 Kanawha. At the northern end of the basin in Marion, Monongalia, 
 Greene, Washington, Fayette, and Westmoreland Counties, limestone 
 forms about one-half of the rock material, and the same is true on the 
 
 N 
 
 western side in Brooke, Ohio, Marshall, and Belmont Counties. Red 
 shale is unknown in the series at the north, but in passing southward 
 from Harrison and Lewis Counties the limestones practically disap- 
 pear, and with them all of the coals except the Pittsburgh. With 
 their disappearance red shales come in and apparently replace the 
 limestones, so that on the Great Kanawha nearly one-fourth of the 
 rock material in this series is red shale, while the thickness is reduced 
 to 270 feet. Along with this change in the character of the rocks 
 there occurs a great change in the topography made by these beds, for 
 at the north, where limestone is abundant, sandstones are few and 
 shaly, so that a gentle, rolling topography results, with a very rich soil 
 and one of the finest grazing and farming regions in the country, while 
 to the southwest, after the limestones have disappeared the sand- 
 stones thicken up and become more massive, thus giving rugged and 
 precipitous slopes with narrow valleys. 
 
 43 
 
44 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 The character of the Upper Coal Measure rocks in the several portions 
 of the area they occupy is shown by the several sections which follow. 
 Section in Fayette and Westmoreland Counties , Pennsylvania. — Prof. 
 
 Stevenson, who has done so much to elaborate the 
 detailed structure of this series, gives the following 
 (Fig. 11), in Second Geological Survey, Pennsylvania, 
 Eeport KK, page 31, as the general section of these 
 beds in Fayette and Westmoreland Counties : 
 
 
 
 
 Fayette and Westmoreland Counties, Pennsylvania. 
 
 [See map, K n.] 
 
 \t£ 
 
 1. Coal, Waynesburg 
 
 2. Sandy shales or sandstone 
 
 3. Coal. Little Waynesburg .. 
 
 4. Limestone, Waynesburg... 
 
 5. Shale and shaly sandstone 
 
 6. Coal, TJniontown 
 
 7. Limestone, TJniontown 
 
 8. Sandstone 
 
 9. Limestone, “ Great” 
 
 10. Coal, Sewiekley 
 
 11 Sandstone 
 
 12. Limestone, Sewiekley 
 
 13. Shale or shaly sandstone... 
 
 14. Coal, Redstone 
 
 15. Limestone, Kedstone 
 
 16. Sandstone or shale 
 
 17. Coal, Pittsburgh 
 
 Ft. 
 
 20 
 
 2 
 
 20 
 
 50 
 
 12 
 
 30 
 
 80 
 
 30 
 
 25 
 
 20 
 
 10 
 
 40 
 
 Ft. 
 
 92 
 
 122 
 
 75' 
 
 Total . 
 
 367 
 
 Section at Broicnsville , Pennsylvania . — At Browns- 
 ville, Fayette County, Pennsylvania, 
 
 Prof. Stevenson finds the following 
 structure, (Fig. 12), for this series, as 
 given in KK, page 233 : 
 
 Fig. 11.— Section in 
 Fayette and West- 
 moreland Coun- 
 ties, Pa. 
 
 Brownsville, Fayette County, Pennsylvania. 
 
 [See map, K m.] Ft. in. 
 
 1. Coal, Waynesburg, blossom 
 
 2. Shales, sandy 45 
 
 3. Coal, Little Waynesburg, blossom 0 
 
 4. Limestone. Waynesburg 4 
 
 5. Shales and shaly sandstone 55 
 
 6. Coal, Uniontown, blossom 
 
 7. Limestone, coarse, yellow 1 
 
 8. Clay 3 
 
 9. Shale and sandstone 16 
 
 10. Limestone 2 
 
 11. Concealed 17 
 
 12. Sandstone 3 
 
 13. Limestone with shales 42 
 
 14. Concealed 16 
 
 15. Limestone 6 
 
 16. Concealed 7 
 
 17. Clay shale 8 
 
 18. Sewiekley coal horizon 
 
 19. Sandy shale and flaggy sandstone 30 
 
 20. Limestone 30 
 
 21. Shale 35 
 
 22. Coal, Kedstone 
 
 23. Shale, sandy 
 
 (Coal.... O' 8" 
 
 24. Coal, Pittsburgh < Clay O' 10" 
 
 (Coal ..7' 6" 
 
 Total 
 
 354 
 
 Fig. 12.— Section at 
 Brownsville, Pa. 
 
GEOLOGICAL SURVEY 
 
 UPPER COAL MEASURES CAPPED WITH PERMO-CARBONIFEROUS BEDS, WHEELING, WEST VIRGINIA. 
 
* THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
WHITE.] 
 
 SECTION AT RICE’S LANDING, PA. 
 
 45 
 
 Section at West Brownsville , Pennsylvania . — On the opposite side of 
 the Monongaliela Biver, in descending from Kreb’s Knob to West 
 Brownsville, in Washington County, the writer meas- 
 ured the several members of this series with the fol- 
 lowing results (Fig. 13) : 
 
 40' 
 
 96'6" 
 
 West Broivnsville, Washington County , Pennsylvania . 
 
 fSee map, K m.] 
 
 ( Coal . 
 
 Coal, Waynesburg ' Clay 0' 
 
 its' 
 
 
 Ft. in. 
 
 .0' 10 
 
 , 3 
 
 ( Coal 2' 6 
 
 Shales and sandstone 45 
 
 Bitumenous shale. Little Waynesburg Coal 1 
 
 Limestone, Waynesburg.-. 10 
 
 Sandstone, shaly 40 
 
 Coal, Uniontown 
 
 Limestone, Uniontown 12 
 
 Shale and sandstone 28 
 
 Limestone, with thin shales .... 88 
 
 Coal, Sewieklev, blossom 
 
 Sandstone, shaly 32 
 
 Limestone 30 
 
 Shales 20 
 
 Coal, Redstone 
 
 Sandstone and shales 
 
 fCoaL.O' 3"] 
 
 Coal, Pittsburgh, roof <j ‘ J', | 2 
 
 (ciay.-l' 0"J 
 
 Coal, Pittsburgh, main bench 7 
 
 6 I 
 
 Ft. in. 
 
 3 7 
 
 96 6 
 
 3 
 
 128 
 
 82 
 
 Total. 
 
 9 6 
 
 308 7 
 
 
 Fig. 13.— Section at 
 West Brownsville, 
 Pa. 
 
 Section at Bice’s Landing , Pennsyl- 
 vania. — In the steep hillside, one mile 
 below Bice’s Landing, Greene County, 
 Pennsylvania, the series exhibits the 
 following structure (Fig. 14) : 
 
 Rice' 8 Landing, Greene County, Pennsylvania. 
 
 [See map, K m.] 
 
 Ft. in. Ft. in. 
 
 fCoal. 
 
 ...V 
 
 0" 
 
 1 Clay. 
 
 ...0' 
 
 5" 
 
 1. Waynesburg coal... < Coal. 
 
 ...r 
 
 3" 
 
 1 Clay. 
 
 ...r 
 
 2" 
 
 [Coal. 
 
 ...2' 
 
 6" 
 
 2. Shales 40 
 
 3. Limestone, Waynesbnrg 6 
 
 4. Shales and sandstone 45 
 
 5. Coal, Uniontown 
 
 6. Limestone, Uniontown 6 
 
 7. Shales and sandstone 38 
 
 8. Limestone, “ Great ” 82 
 
 9. Coal, Sewickley , 
 
 10. Sandstone 40 
 
 11. Limestone 25 
 
 12. Sandy shale 30 
 
 13. Slate, bituminous (Redstone coal) 
 
 14. Sandstone, Pittsburgh, flaggy 15 
 
 15. Sandstone, Pittsburgh, massive 30 
 
 ( C Coaly shale 
 
 [ Roof. < Coal 
 
 16. Coal, Pittsburgh.. . ^ f. Clay 
 
 { Main bench 7' 
 
 Total 
 
 6 4 
 91 
 
 1 6 
 126 
 1 9 
 95 
 1 6 
 45 
 
 10 
 
 378 1 
 
 fjgiill 
 
 6V 
 
 ifUii 
 
 4& 
 
 a* 
 
 =• =r— — 
 
 6 
 
 
 4S' 
 
 
 i'6"J 
 
 
 6' 
 
 
 3&' 
 
 , ■ ■ • ; • ; g 
 
 
 
 
 KBS 
 
 82' 
 
 
 
 
 if ; 
 
 ; S 
 
 4 O' 
 
 
 25’ 
 
 ■ 
 
 
 3 O’ 
 
 
 l’6\ 
 
 15’ 
 
 
 
 30 
 
 SSlISSffi 
 
 io’ 
 
 
 Flo. 14.— Section at 
 Rice’s Landing, Pa. 
 
46 THE NORTHERN BITUMINOUS COAL FIELD. [bull. 65. 
 
 Section on Robinsorts Run . West Virginia. — The Upper Goal Measure 
 beds attain a very fine development in Monongalia County, West 
 Virginia, just south from the Greene County line, and there, on Eobin- 
 son’s Eun, 2 miles west from the Monongahela Eivefc, the following 
 succession (Fig. 15) is exposed : 
 
 
 
 
 33? 
 
 
 ft 
 
 O* 
 
 f 
 
 
 40’ 
 
 ijjgjgg 
 
 3" 
 
 a' 
 
 
 
 
 
 
 5 
 
 7 : : ■ : 
 
 * 
 
 
 sf 
 
 1 
 
 i 
 
 f 
 
 10' 
 
 SIM* 
 
 * 
 
 
 
 |Mll 
 
 is' 
 
 A 
 
 K>' 
 
 20' 
 
 IHHHfldl 
 
 9. 
 
 a* 
 
 Fig. 15. — Section on 
 Bobinson’s Kun, 
 W. Va. 
 
 Bobinson’s Bun, Monongalia County , West Virginia. 
 
 [See map, L m.] 
 
 Ft. in. 
 
 f Coal... 2' 6” 
 
 1. Coal, Waynesburg . . < Shale. .1' 6" 
 
 ( Coal . .4' 0" 
 
 2. Sandy shales with iron ore below middle 35 
 
 3. Limestone, Waynesburg 8 
 
 4. Shales 10 
 
 5. Limestone *. 1 
 
 6. Sandstone, flaggy 40 
 
 7. Black slate (Uniontown coal) 5 
 
 8. Limestone, Uniontown 10 
 
 9. Sandstone and shales 35 
 
 10. Limestone 6 
 
 11. Shales 10 
 
 12. Sandstone, flaggy 30 
 
 13. Limestone, cement beds 20 
 
 14. Sandstone,' "Sewickley 35 
 
 15. Coal, Sewickley 
 
 16. Shales 10 
 
 17. Limestone 10 
 
 18. Shales 12 
 
 19. Limestone 18 ‘ 
 
 20. Shales 15 
 
 21. Coal, Bedstone 
 
 22. Limestone, Bedstone 10 
 
 23. Shales and slates 20 
 
 24. Coal, Pittsburgh. 
 
 ( Boof coals - .3' ) 
 
 \ Clay l'[ 
 
 (Coal 8' ) 
 
 Ft. in 
 
 8 
 
 94 
 
 151 
 
 65 
 
 30 
 
 12 
 
 Total 
 
 Here, as will be seen from the above section, the Eedstone coal, 
 which belongs between the Pittsburgh and Sewickley beds, has thick- 
 ened up into merchantable condition. This coal contains a little more 
 sulphur than either the Pittsburgh below or the Sewickley above, but 
 it makes a very fair fuel for domestic and steam producing purposes. 
 It is softer than either of the other two and would coke well. 
 
 The Eedstone, Pittsburgh, and Sewickley beds of this section foot 
 up a total thickness of 21 J feet, including partings, and about 17 feet 
 of this is merchantable coal. 
 
WHITE.] 
 
 SECTION ON SCOTT’S RUN, WEST VIRGINIA. 47 
 
 Section on Scotfs Run , West Virginia . — A short distance south from 
 Robinson’s Run, we get another fine exposure of the Upper Coal Meas- 
 ure beds along the waters of Scott’s Run, between Cassville and the 
 mouth of the stream, as follows (Fig. 16) : 
 
 Scotfs Bun, Monongalia County, West Virginia. 
 
 [See map, M m.] 
 
 1. Coal, Way nesburg. 
 
 2. Black slate. 
 
 os* 
 
 
 Fig. 16. — Section on 
 Scott’s Run, W.Va. 
 
 f Coal 2' 0"1 
 
 f Shale, fossiliferous..l' 0" | 
 
 { Coal 1' 4" > 
 
 | Shale, gray V 6" | 
 
 [Coal 1 5' 0” J 
 
 3. Sandy shales, with iron ore 
 
 4. Limestone, W aynesburg 
 
 5. Sandy shales, with limestone layers 
 
 6. Sandstone, massive 
 
 7. Limestone and shales 
 
 8. Black slate, representing Uniontown coal 
 
 9. Limestones, interstratified with thin shales, cement 
 
 beds near base 
 
 10. Sandstone, Sewickley 
 
 11 . Coal, Sewickley 
 
 12. Shales 
 
 13. Sandstone 
 
 14. Limestone - 
 
 15. Shales, greenish gray 
 
 16. Concealed 
 
 17. Limestone, steel gray 
 
 18. Concealed 
 
 19. Coal, Redstone 
 
 20. Li mestone, Redstone - 
 
 21. Shale and fire clay 
 
 22. Slate, black 
 
 ( Coal. 0' 3" I 
 
 23. Coal, Pittsburgh, roof i CoS!.'? 0" f 
 
 L Clay! . V 0" J 
 
 ( Coal.. 3' 6" 
 
 Slate .0' 
 
 | Coal.. O' 8" 
 
 | Slate. O' 1" 
 
 24. Coal, Pittsburgh, main bench .. ^ Coal. .1' 6" 
 
 [ Slate. 0' 
 
 Coal.. O' 6" 
 
 I Slate. 0' | 
 
 l Coal.. 3' 3" J 
 
 Total 
 
 Ft. in. 
 
 Ft. in. 
 10 10 
 
 105 
 
 40 
 
 5 
 
 10 
 
 5 
 
 8 
 
 15 
 
 7 
 
 15 
 
 18 
 
 5 
 
 5 
 
 2 
 
 145 
 
 5 
 
 65 
 
 4 
 
 28 
 
 13 10£ 
 
 9 7i 
 
 372 8& 
 
 The same Redstone coal makes its appearance in this section ; in fact 
 it underlies all of the region intervening between Scott’s and Robin- 
 son’s Runs, thinning out southward as well as northward. It underlies 
 an area of probably 5,000 acres where it is of workable thickness. In 
 the oil-well borings on Doll’s Run, and as far west as Mannington and 
 Fairview, this bed is still present, though apparently not of workable 
 thickness. 
 
48 
 
 THE NORTHERN BITUMINOUS COAL FIELD, 
 
 [BULL. 65. 
 
 Section on Buffalo Creek , West Virginia . — Along Buffalo Creek, in 
 the vicinity of Fairmont, Marion County, West Virginia, the Upper 
 Coal Measures exhibit the following succession (Fig. 17): 
 
 Buffalo Creek, Marion County , West Virginia. 
 
 [See map, M 1.] 
 
 f Coal... O' 6" 1 
 i Shale.. O' 1" | 
 
 1. Coal, Waynesburg •( Coal. . 1' 0" V ... 
 
 I Shale.. 1' 4" 
 
 1 Coal. ..3' 0'' J 
 
 2. Shales 
 
 3. Sandstone, massive 
 
 4. Shale 
 
 5. Limestone, Waynesburg 
 
 6. Shales 
 
 7. Limestone 
 
 Fig. 17. — Section on 
 Buffalo Creek, W. Va. 
 
 8. Shales r 
 
 9. Sandstone 
 
 10. Shales 
 
 11. Coal, Uniontown 
 
 12. Fire clay 
 
 13. Sandstone 
 
 14. Shales and black slate 
 
 15. Limestone 
 
 16. Fire clay 
 
 17. Shales with limestone 
 
 18. Sandstone 
 
 19. Blue shale 
 
 20. Limestdfre 
 
 21. Shales and concealed 
 
 22. Limestone interstratified with thin shales 
 
 23. Shales 
 
 fCoal 5' 0"1 
 
 I Clay O' 4' j 
 
 24. Coal, Sewickley Coal 0' 4" } .. 
 
 I Slate, dark .0' 3" J 
 
 [Coal O' 5" j 
 
 25. Shales 
 
 26. Limestone, buff 
 
 27. Sandstone, gray, massive 
 
 28. Limestone, gray 
 
 29. Concealed and shales 
 
 30. Impure clay 
 
 31. Limestone and shales 
 
 32. Sandstone, Pittsburgh 
 
 33. Shales 
 
 f Coal, bony. 0' 10" 1 
 
 I Bone O' l\" 
 
 I Coal 2' 3" 
 
 34. Coal, Pittsburgh. . . Slate 0' i" } 
 
 I Coal 0' 5" 
 
 [Slate 0' i"| 
 
 [Coal 3' 5£" J 
 
 Total 
 
 !. in. Ft. in. 
 
 5 11 
 
 20 
 
 30 
 
 3 
 
 1 6 
 18 
 
 1 6 
 12 
 10 
 5 
 
 4 
 1 
 
 5 
 3 
 5 
 5 
 2 
 
 > 101 
 
 2 6 
 
 149 
 
 1 
 
 25 
 
 85 
 
 5 
 
 J 
 
 6 4 
 
 3 6 
 
 4 
 18 
 
 5 
 
 15 
 
 5 
 
 20 
 
 25 
 
 5 
 
 100 6 
 
 I 
 
 7 1* 
 
 372 4$ 
 
 The portion of this section from the Sewickley coal down to the base 
 of the series was measured at the Montana mines, 2J miles below the 
 mouth of Buffalo Creek. 
 
 The Redstone coal is entirely absent here, its horizon being occupied 
 by the 5 feet of impure fire clay, 50 feet above the Pittsburgh bed. 
 
 Section at Clarksburg , West Virginia . — In passing from Marion County 
 southward towards Clarksburg, in Harrison County, a great change 
 takes place in the character of the sediments of the Upper Coal Meas- 
 
WHITE.] 
 
 SECTION AT WHEELING, W. VA. 
 
 49 
 
 ures. The limestones, so prominent in Greene, Monongalia, and 
 Marion, dwindle down to insignificant proportions, as shown by the fol- 
 lowing section (Fig. 18), made at Clarksburg by Mr. Jno. L. Johnston, 
 civil engineer : 
 
 Clarksburg, Harrison County, West Virginia. 
 
 Fig. 18.— Section at 
 Clarksburg, W. Va. 
 
 [See map, Ok.] 
 
 1. Waynesburg coal, absent or not seen 
 
 2. Concealed and yellow sandy shales 65 
 
 3. Sandstone 25 
 
 4. Concealed, with some limestone - 80 
 
 5. Sandstone 20 
 
 6. Concealed 5 
 
 7. Sandstone 15 
 
 8. Sandy shales 6 
 
 9. Sandstone, Sewickley 25 
 
 10. Shales 10 
 
 11. Coal, Sewickley 
 
 12. Limestone {lood":# 6"}“" 9 
 
 13. Concealed 3 
 
 14. Shales, sandy 14 
 
 15. Shale, with iron nodules 1 
 
 16. Shales, sandy 4 
 
 17. "Sandstone 1 
 
 18. Concealed 8 
 
 19. Coal, Redstone, slaty 
 
 20. Shale, dark, bituminous 5 
 
 21. Limestone, Kedstone 6 
 
 22. Shale, greenish 13 
 
 23. Slate, bituminous , 1 
 
 ( Coal 3 5' 
 
 24. Coal, Pittsburgh . { Bone ... O' 1 
 
 Ft. in. 
 
 I Coal 5' 0‘ 
 
 
 Ft. in. 
 0 
 
 > 251 
 
 40 
 
 Total 
 
 328 6 
 
 Section at Cliapline Hill , Wheeling , West Virginia . — Between the Monon- 
 
 gahela and Ohio Rivers a considerable change takes place 
 in the character of the Upper Coal Measure beds, and 
 also in the thickness of the several members, as will be 
 seen by the following section (Fig. 19) from Chapline 
 Hill, Wheeling, West Virginia: 
 
 Chapline Hill, Wheeling, West Virginia. 
 
 Ft. in. 
 
 1 
 
 [See map, K j.] 
 
 1. Coal, Waynesburg ' 
 
 2 . Concealed 5 
 
 3. Flaggy sandstone, filled with plant fragments 4 
 
 4. Concealed 4 
 
 5. Limestone, shales and concealed 60 
 
 6 . Sandstone, massive, gray 5 
 
 7. Limestone and concealed 20 
 
 8 . Green shale 5 
 
 9. Limestone, interstratified with shales 55 
 
 C Coal . . 1 
 
 10. Coal, Sewickley. < Sandy shales with plants 12 
 
 ( Cos ’ 
 
 Ft. in. 
 2 
 
 158 
 
 11. Sbales 8 
 
 12. Sandstone, rather massive, micaceous, current-bedded 20 
 
 13. Limestone, impure, flaggy, filled with fossil ferns 1 
 
 14. Coal, Redstone 
 
 15. Limestone, mostly bnffish and impuro. 
 
 C Coal, roof 2' ' 
 
 16. Pittsburgh coal < Shale 
 
 ( Coai, main bench. 
 
 0 ) 
 ! 
 
 1 
 
 13 8 
 
 29 
 
 0 10 
 55 
 
 60' 
 
 15tf 
 
 20 ' 
 
 Total 
 
 Bull. 65- 
 
 267 
 
 Fig. 19.— Section at 
 — Chap lino Hill, 
 6 Wheeling, W.Va. 
 
50 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Here the Waynesburg coal has dwindled to an unimportant bed, 
 and the Sewickley has split into two portions separated by 12 feet of 
 shales, while the whole column has lost more than 100 feet of thick- 
 ness compared with the Monongahela River region. 
 
 Section near Bellaire , Ohio . — At Bellaire, Ohio, 4 miles below Wheel- 
 ing, the following carefully leveled section (Fig. 20) was made by Prof. 
 0. N. Brown, of the present Ohio Geological Survey. It exhibits some 
 interesting changes as compared with the Wheeling section : 
 
 Near Bellaire , Belmont County, Ohio. 
 
 [See map, K i.] 
 
 Ft. in. Ft. in. 
 
 1. Coal, Waynesburg 
 
 2. Shale, sandy 
 
 3. Shale 
 
 4. Limestone 
 
 5. Concealed 
 
 6. Coal, blossom, Little Waynesburg 
 
 7. Concealed 
 
 8. Coal, blossom, Uuiontown 
 
 9. Shale 
 
 10. Sandstone 
 
 11. Shale, argillaceous 
 
 12. Concealed...... : 
 
 13. Shale 
 
 14. Sandstone - 
 
 15. Shale 
 
 16. Concealed 
 
 17. Calcareous shale, -with thin limestones 
 
 f Coal 4' 0"1 
 
 j Shales, sandy 13' 10" ! 
 
 18. Coal, Sewickley Coal O' 8" } ... 
 
 | Shale, argillaceous 6' 0" } 
 
 l Coal -. 3' 0" J 
 
 19. Shale, argillaceous 
 
 20. Limestone, thin clay in center 
 
 21. Limestone, magnesian, cement rock 
 
 22. Clay 1 
 
 23. Limestone 
 
 24. Concealed 
 
 25. Coal, Redstone, blossom 
 
 26. Concealed 
 
 27. Shale - 
 
 28. Coal, Pittsburgh 
 
 Pig. 20. — Section near 
 
 Bellaire, Ohio. Total 
 
 6 
 
 12 
 
 3 
 
 5 
 
 14 
 
 4 
 
 6 
 
 20 
 
 32 
 2 
 3 
 3 
 
 33 
 
 24 6 
 
 2 
 
 8 
 
 5 
 
 1 
 
 11 
 
 11 
 
 17 
 
 1 
 
 <1 
 
 2 
 
 40 
 
 J 
 
 1 
 
 127 6 
 
 27 6 
 
 38 
 
 2 
 
 18 
 
 7 
 
 263 
 
 The interval between the two members of the Sewickley coal has 
 here increased to 20 feet, and the upper one seems to keep permanently 
 above the lower one from here southwest ward through Ohio, becoming 
 the Cumberland and Meigs Creek bed of the Ohio geologists. 
 
 Both the Little Waynesburg and Uniontown coals are represented 
 in this section, but neither one was observed at Wheeling. 
 
 It is worthy of note that there is a difference of only 4 feet in the 
 total thickness of the Upper Coal Measures as given by Prof. Brown’s 
 section at Bellaire and mine at Wheeling, four miles above. 
 
BULLETIN NO. 65 PL. 
 
 UPPER COAL MEASURES AND PERMO-CARBONIFEROUS, POWHATAN, OHIO. 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
WHITE. 1 
 
 SECTION ON PIPE CREEK, OHIO. 
 
 51 
 
 Section at Moundsville , West Virginia .—* Near the mouth of Grave 
 Creek, one mile below Moundsville, West Virginia, and 7 miles below 
 Bellaire, these measures exhibit the following succession by combining 
 the surface exposures with the record of an oil boring (Fig. 21) : 
 
 zo- 
 
 Fig. 21. — Section at 
 Moundsville, W. Va. 
 
 Moundsville , Marshall County , West Virginia. 
 
 [See map, K i.] 
 
 Ft. in. 
 
 l Coal, impure . . 0 ' 6" ) 
 
 1. Coal, Waynesburg < Shale V 0" > 
 
 ( Coal V 6") 
 
 2. Shale, soft, gray 5 
 
 3. Sandstone, massive, gray, micaceous 20 
 
 4. Concealed, with limestone layers at base 2 feet thick 20 
 
 5. Flaggy sandstone and sandy shales 20 
 
 6. Concealed 10 
 
 7. Limestone 1 
 
 8. Concealed 14 
 
 9. Limestone, gray 22 
 
 10. Concealed to mouth of oil and gas well at 30 feet above 
 
 low- water mark in Ohio Fiver 28 
 
 11. Conductor hole of oil-well record 18 
 
 12. Limestone, light gray 40 
 
 13. Slate • 15 
 
 14. Black rock, shales 10 
 
 15. Coal, Bedstone : 
 
 16. Fire clay 7 
 
 17. Hard slate 4 
 
 18. Gray limestone 20 
 
 19. Bastard limestone 10 
 
 20. Coal, Pittsburgh 
 
 Ft in. 
 3 
 
 223 
 
 Total 
 
 274 6 
 
 Section on Pipe Greek , Ohio . — Pipe Creek puts into the Ohio Eiver 
 3 miles below the mouth of Grave Creek, and there, on the Belmont 
 County side of the river, the Pittsburgh coal is at low-water level. The 
 following structure (Fig. 22) is found in the steep hills which border 
 the mouth of Pipe Creek : 
 
 Pijje Creek , Belmont County , Ohio. 
 
 [See map, K i.] 
 
 1. Coal, Waynesburg, slaty at top 
 
 2. Concealed, limestone and shales 
 
 3. Bituminous slate, Uniontown coal 
 
 4. Limestone, Uniontown 
 
 5. Concealed, with much limestone 100 
 
 Coal, and coaly shale. 
 
 2' 
 
 0" 
 
 Sandstone 
 
 !l2' 
 
 0" 
 
 Coal 
 
 . O' 
 
 4" 
 
 Shale 
 
 . 1' 
 
 0" 
 
 Coal 
 
 
 4" 
 
 Shale, sandy 
 
 . 5' 
 
 0" 
 
 Coal, slaty 
 
 . 1' 
 
 8" 
 
 Shale 
 
 . O' 
 
 4" 
 
 Coal 
 
 . 1' 
 
 0" 
 
 Black slate 
 
 . 0' 
 
 4" 
 
 7. Limestone, Sewickley, and. shales 
 
 8. Bituminous shale, (Redstone coal) ... 
 
 9. Limestone, (Redstone)and concealed. 
 
 10. Coal, Pittsburgh 
 
 Total. 
 
 Feet. 
 
 Feet. 
 
 4 
 
 
 55 
 
 
 1 
 
 .. 10 i 
 
 i 110 
 
 
 24 
 
 
 22 
 
 
 1 
 
 
 25 
 
 
 6 
 
 
 248 
 
 Fig. 22.— Section in 
 Bel m out County, 
 Ohio. 
 
52 
 
 [BULL. 65 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 Below this last locality no measurement of the Upper Coal Measure 
 series is possible for a long distance, because most of the members are 
 below water level. They are all brought to the surface, however, by 
 the Volcano anticline, which crosses the Ohio River from Pleasants 
 County, West Virginia, into Washington County, Ohio. 
 
 Section in Washington County , Ohio . — Mr. F. W. Minshall, of Marietta, 
 Ohio, has made a very careful study of these measures in Washington 
 County, Ohio, and has prepared the followiug section (Fig. 23) as rep- 
 resenting their usual structure there : 
 
 Washington County , Ohio. 
 
 [See map, M g.J 
 
 Fig. 23. — Section in 
 Washington County, 
 Ohio. 
 
 1. Coal, Waynesburg (Macksburg) 
 
 2. Shale 
 
 3. Sandstone 
 
 4. Shale 
 
 5. Limestone 
 
 6. Shaly sandstone 
 
 7. Limestone and shale 
 
 8. Coal, Sewickley (Meigs Creek) . . 
 
 9. Shales and limestone 
 
 10. Shales . 
 
 11. Sandstone 
 
 12. Shales 
 
 13. Coal, Pittsburgh, thin .. 
 
 Total 
 
 Ft. in. Ft. in. 
 
 14 
 
 11 
 
 18 
 
 6 
 
 18 
 
 29 
 
 25 
 
 40 
 
 19 
 
 4 
 
 4 
 
 > 96 
 
 2 6 
 
 190 6 
 
 The thickness here given is 50 to 60 feet less for the entire series than 
 that usually found in any other portion of the Appala- 
 chian field. 
 
 Section at Burning Springs , West Virginia. — In the vi- 
 cinity of Burning Springs, Wirt County, West Virginia, 
 these rocks are brought above the surface by the same 
 anticline, and there Mr. Minshall reports the following 
 structure (Fig. 24) : 
 
 Burning Springs, Wirt County, West Virginia. 
 
 ' Z07' 
 
 [See map, P g.] 
 
 1. Coal, Waynesburg 
 
 2. Concealed and shales 
 
 3. Sandstone, Pittsburgh 
 
 4. Shales 
 
 5. Coal, Pittsburgh 
 
 Ft. in. 
 1 8 
 
 207 
 
 30 
 10 
 1 8 
 
 250 4 
 F 
 
 'lG. 24. — Section ;it. 
 Burning Springs 
 W. Va, 
 
 Total 
 
White. 1 
 
 SECTION AT ANTIQUITY, OHIO. 
 
 53 
 
 Both here and all along the Volcano anticline the Pittsburgh coal 
 is very poorly developed, as shown in this and the previous section, 
 and it is frequently absent entirely. 
 
 Section on Leading Creelc , West Virginia.— Near Leading Creek post- 
 office, at the eastern edge of Gilmer County, West Virginia, this series 
 shows thus (Pig. 25) : 
 
 Fig. 25.— Section on 
 Leading Creek, W.Va. 
 
 Leading Creelc , Gilmer County , West Virginia. 
 
 [See map, P j.] 
 
 Feet. 
 
 1. Waynesburg coal horizon (absent) 0 
 
 2. Shales 10 
 
 3. Limestone, brecciated 3 
 
 4. Shales and concealed ». 35 
 
 5. Sandstone, yellow, massive, soft, pebbly 40 
 
 6. Shales 10 
 
 7. Limestone, impure 2 
 
 8. Shales 40 
 
 9. Sandstone, massive 40 
 
 10. Shales 55 
 
 | Coaly shales . . 2' 0" 1 
 | Clay 0' 10" 1 
 
 11. Coal,Pittoburgh...(g»^f» al ::; »; «;![ 8 
 
 ! Bony slate o' 4" |~ 
 
 [ Coal 2' 0"J 
 
 Total 243 
 
 Section at Antiquity , Ohio. — Along the Ohio River, below where the 
 Volcano arch crosses, the Upper Coal Measures again plunge under 
 water level, and do not emerge again till we come to the 
 vicinity of Antiquity, Meigs County, Ohio, 100 miles be- 
 low. A shaft to the Pittsburgh bed (130 feet under river 
 level), taken in connection with the surface exposures 
 there, reveals the following succession (Fig. 26) : 
 
 Antiquity , Meigs County, Ohio. 
 
 [See map, P e.] 
 
 Ft. in. 
 
 L Waynesbnrg coal (absent) 0 
 
 2. Shales and sandstones 172 
 
 3. Sandstone, massive, Pittsburgh 70 
 
 4. Shales, with fossil plants 10 
 
 (Coal 2' G") 
 
 5. Coal, Pittsburgh < Slate O' 2" > 5 g 
 
 (Coal 3' 0") 
 
 Total 257 8 
 
 Fig. 26. — Section 
 at Antiquity, Ohio. 
 
 Section at Hartford City , West Virginia,— Six miles below the shaft 
 at Antiquity, and in the vicinity of Hartford City, the Pittsburgh coal 
 
54 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 comes above water level. In the steep bluffs above Hartford the fol- 
 lowing succession (Fig. 27) was observed : 
 
 
 Hartford City, Mason County , West Virginia . 
 
 
 70 
 
 [See map, P d.] 
 
 Ft. in. 
 
 1. Waynesburg coal (absent) 0 
 
 2. Red shale 10 
 
 3. Shale, gray 5 
 
 4. Sandstone 6 
 
 5. Shales, brown, sandy 10 
 
 6. Shales, red 2 
 
 7. Concealed 14 
 
 8. Red shale, with limestone nodules 10 
 
 9. Sandstone 20 
 
 10. Shales, variegated with limestone nodules near base 28 
 
 11. Concealed... - 20 
 
 12. Red shale 5 
 
 13. Concealed 20 
 
 14. Shale, red 15 
 
 15. Sandstone, massive, Pittsburgh 70 
 
 16. Shales, gray, fossil plants 15 
 
 17. Coal, Pittsburgh 5 6 
 
 Total 255 6 
 
 i 
 
 Fig. 27. — Section at 
 Hartford City, 
 
 W.Va. 
 
 Section at Arbuckle , West^ Virginia .— In the vicinity of Arbuckle, 
 Mason County, West Virginia, on the Great Kanawha River, and 18 
 miles above its mouth, the Waynesburg coal makes its appearance in 
 the section. Here the following structure (Fig. 28) was obtained for 
 the series, by combining the surface exposures with the record of a 
 boring made by Mr. Craig : 
 
 Arbuckle, Mason County, West Virginia. 
 
 [See map, Q e.) 
 
 1. Waynesburg coal 
 
 f Coal, slatv 
 
 ..O' 
 
 10" 
 
 | Coal, sulphurous . 
 
 ..O' 
 
 8" 
 
 <( Shale, dark 
 
 ..0' 
 
 5" 
 
 | Coal, good 
 
 ..O' 
 
 8" 
 
 ( Coal, slaty 
 
 ..0' 
 
 5" 
 
 2. Shales, sandstone, and concealed 
 
 3. Sandstone, blue 
 
 4. Shales, red 
 
 5. Sandstone, blue, hard 
 
 6. Variegated shales 
 
 7. Coal, Sewickley 
 
 8. Sandstone 
 
 9. Shales, red 
 
 10. Shales, variegated 
 
 11. Fire clay, impure (Redstone coal) 
 
 12. Sandstone, coarse, white, Pittsburgh 
 
 13. Fire clay and shale with a little slaty coal at bottom, Pittsburgh. 
 
 Ft. 
 
 150 
 
 4 
 
 2 
 
 14 
 
 8 
 
 1 
 
 6 
 
 4 
 
 48 
 
 2 
 
 29 
 
 10 
 
 
 
 Total . 
 
 Fig. 28.— Sect 
 at Arbuckle, 
 281 Va. 
 
 ion 
 , W. 
 
 Here there is practically no merchantable coal in the whole series, 
 since the Waynesburg bed, although 3 feet thick, is poor and slaty. 
 
WHITE.] 
 
 SECTION OPPOSITE WINFIELD, W. VA. 55 
 
 The locality is near the center of the deepest portion of the Appalachian 
 trough, and the horizon of the Pittsburgh coal is 90 feet under the Ka- 
 nawha. A hole was drilled as a test for. this coal, but the result proved 
 
 only a trace of it present. 
 
 Section at mouth of Big Hurricane Creek , Putnam County , West Vir- 
 ginia. — Southward up the Kanawha River from Arbuckle, the locality 
 of Section 28, the rocks rise and the entire series comes above water 
 
 level at the mouth of Big Hurricane Greek, in Putnam County. Here, 
 32 miles from the mouth of the Big Kanawha, the fol- 
 lowing succession may be seen (Fig. 29) : 
 
 
 mm 
 
 -"••-••I 
 
 TfsYVtYVYYY. 
 
 Mouth of Big Hurricane Creek, Putnam County, West Virginia. 
 
 [See map, R d.] 
 
 Ft. in. 
 
 1. Waynesburg coal (absent) - 0 
 
 2. Shales, red and sandy 35 
 
 3. Sandy shales 20 
 
 4. Sandstone, massive . . 30 
 
 5. Coal, Uniontown 0 G 
 
 6. Red shales, with limestone 10 
 
 7. Shales, sandy 10 
 
 8. Concealed 10 
 
 9. Shales, sandy 10 
 
 10. Concealed and red shales 20 
 
 11. Sandstone, massive 20 
 
 12. ' Concealed 20 
 
 13. Sandstone, massive 35 
 
 14. Shale, with iron ore 12 
 
 15. Sandstone 18 
 
 [Coal 0' 10" 1 
 
 Shales 5' 0" | 
 
 16. Coal, Pittsburgh, roof <j l^dston?. ! ! 1' 8" 
 
 I Slate, black . . 2' 0" 
 
 (Fireclay V 3' 
 
 11' 9") 
 I 
 I 
 
 15 8 
 
 Fig. 29. — Section at 
 mouth of Big Hurri- 
 cane Creek, W. Va. 
 
 C Coal 3' 3") 1 
 
 Coal, Pittsburgh, main bench. < Slate 0' 2" > 3' 11" J 
 
 l Coal 0' 6" S 
 
 Total 266 2 
 
 The Pittsburgh coal is patchy all through this region, 
 being workable on some farms and absent on others. 
 
 Section opposite Winfield , West Virginia. — As showing 
 the unreliable character of the coals in this series along 
 this portion of the Kanawha, the section (Fig. 30) of the 
 rocks opposite Winfield, Putnam County, 5 miles above 
 Big Hurricane, is given : 
 
 Opposite Winfield, Putnam County, West Virginia. 
 
 [See map, So.] 
 
 Ft. 
 
 1. Waynesburg coal (absent) 0 
 
 2. Shales, red, with limestone nodules 5 
 
 3. Sandstone, shaly 10 
 
 4. Concealed 10 
 
 5. Red shale 10 
 
 6. Sandstone, flaggy 30 
 
 7. Red shales, with limestone 10 
 
 8. Sandstone, shaly 20 
 
 9. Red shale - 25 
 
 10. Sandstone, shaly - 10 
 
 11. Red shales 10 
 
 12. Sandstone, flaggy - 10 
 
 13. Concealed 10 
 
 14. Red shale, with limestone nodules near base 15 
 
 15. Sandstones, red, and gray shales 75 
 
 16. Fire clay, place for Pittsburgh coal — 0 
 
 Total 250 
 
 Fig. 30. — Section 
 opposite Win* 
 lield, W. Va. 
 
56 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 This section was measured in the steep hill at Red House Station, on 
 the Kanawha and Ohio Railroad, and, as may be seen, the series does 
 not there contain any coal whatever. 
 
 Section near Raymond City, West Virginia.— Further up the Kanawha 
 the Pittsburgh coal again comes in, and the follow- 
 ing structure (Fig. 31) is found in the vicinity of 
 Raymond City, 6 miles above Winfield : 
 
 30' 
 
 Near Raymond City , Putnam County , West Virginia. 
 
 [See map, S e,] 
 
 Ft. in. 
 
 1. TVaynesburg coal (absent) 0 
 
 2. Concealed, with red shale 60 
 
 3. Red shale 30 
 
 4. Sandstone, gray, micaceous 4 
 
 5. Limetone, in red shale 5 
 
 6. Red shale 15 
 
 7. Sandy shale, gray 30 
 
 8. Shale, red 40 
 
 9. Sandy shales, yellowish gray 45 
 
 10. Black shale, Redstone coal 2 
 
 11. Sandstone, Pittsburgh 40 
 
 12. Shales 10 
 
 ( Coal 0' 4' 
 
 j Shale 0' 4 
 
 13. Coal, Pittsburgh, roof -i g^J e ; ; ; ; ; ; 
 
 | Coal, slaty... V 0' 
 
 [Fine clay V 6' 
 
 Fig. 31. — Section near 
 Raymond City, W. Va. 
 
 L Coal, good 
 
 14. Coal, Pittsburgh, main bench. { ~ m 
 
 0 " 
 
 Slate! 1 0- £ 
 
 (Coal, slaty... 0' 10 
 
 i) ' 
 
 ■s 
 
 6 ' 10 *' 
 
 10 7$ 
 
 Total 291 7* 
 
 Section in vicinity of Western Port , Maryland. — In the Cumberland or 
 Georges Creek basin, the Upper Coal Measures ex- 
 hibit the following structure (Fig. 32), as observed 
 in the vicinity of Western Port, Maryland : 
 
 Vicinity of Western Port, Alleghany County, Maryland. 
 
 [See map, N p.] 
 
 Ft. in. 
 
 1. Waynesburg coal (not seen) 0 
 
 2. Concealed and shales 130 
 
 3. Coal, Sewickley 5 
 
 4. Shales and concealed * 115 
 
 5. Coal, Pittsburgh, roof 
 
 [Coal 
 
 . 0' 
 
 8"' 
 
 j 
 
 ] Shale 
 
 . 4' 
 
 0" 
 
 > 6' 8 " 1 
 
 ) Coal 
 
 
 0" 
 
 1 Shale 
 
 . 1' 
 
 0" J 
 
 1 
 
 [Coal 
 
 .10' 
 
 0" 1 
 
 1 
 
 V 
 
 Slate 
 
 0' 
 
 2" 
 
 ( 
 
 | Coal 
 
 . 0' 
 
 9" 
 
 
 ^ Slate 
 
 . 0' 
 
 
 > 13' 7 i"J 
 
 1 Coal 
 
 . 2' 
 
 0” 1 
 
 | Black slate 
 
 . 0' 
 
 6" I 
 
 
 [ Soft coaly shale 
 
 . O' 
 
 2" J 
 
 1 
 
 20 31 
 
 Total 270 3J 
 
 Fig. 32. — Section 
 near W estern Port, Md. 
 
WHITER 
 
 THE UPPER COAL MEASURES. 
 
 57 
 
 From the foregoing sections it will be perceived that the beds in the 
 
 Upper Coal Measures which have 
 scending order as follows : 
 
 Waynesburg coal. 
 
 Browntown sandstone. 
 
 Little Waynesburg coal. 
 Waynesburg limestone. 
 
 Uniontown sandstone. 
 
 Uniontown coal. 
 
 Uniontown limestone. 
 
 Great limestone. 
 
 received distinct names are in de- 
 
 Sewickley sandstone. 
 Sewickley coal. 
 Sewickley limestone. 
 Redstone coal. 
 Redstone limestone. 
 Pittsburgh sandstone. 
 Pittsburgh coal. 
 
 These several beds we shall now notice more in detail. 
 
 CHARACTERISTIC HORIZONS. 
 
 THE WAYNESBURG COAL. 
 
 This, the highest member of the series, is generally quite persistent 
 around the northern end of the coal field, but followed southward 
 through West Virginia it soon becomes patchy and interrupted, so that 
 beyond the line of Marion County the coal is only occasionally present 
 along the eastern and central portions of the Upper Coal Measure belt, 
 its horizon being frequently occupied, as at Harrisville, Ritchie County 
 by a brecciated limestone. 
 
 On the Great Kanawha this coal occurs near the center of the Appa- 
 lachian trough over a small area in the vicinity of Arbuckle, and its 
 structure there is given in Section 28. 
 
 Along the western side of the field, down the Ohio River and across 
 southern Ohio, this coal is fairly persistent. It dips under the Ohio 
 River at New Martinsville, but rises to daylight again near St. Mary’s, 
 where it is only 1 to 3 feet thick, and quite sulphurous. 
 
 In the Macksburg oil region it is the principal bed, according to the 
 Ohio geologists, and has a thickness of 4 feet. 
 
 This coal is almost universally double, being separated into two layers 
 by a division of shale and slate. This is so common at the northern end 
 of the field that it is known there as the “horse-back” vein. In Mo- 
 nongalia and Greene Counties the bed is often 8 to 10 feet thick and 
 separated into three layers, the upper division of slate being very fos- 
 siliferous, and often, as at Cassville, West Virginia, containing many 
 insect remains, together with fossil plants. 
 
 The coal from this bed is usually rather hard, and comes out in large 
 blocks ; but it frequently contains injurious quantities of sulphur. This 
 renders it unfit for smithing, as well as for the manufacture of coke and 
 gas, but it is generally a useful fuel for steam and domestic jmrposes. 
 
 IRON ORE. 
 
 The shales which underlie the Waynesburg coal sometimes contain 
 a considerable quantity of iron nodules, and they were once mined in 
 
58 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 66. 
 
 Morgan Township, Greene County, Pennsylvania, and used in manu- 
 facturing iron. The same ore occurs near Bethel Church, Cass District, 
 Monongalia County, at 15 to 20 feet below the coal. 
 
 THE BROWNTOWN SANDSTONE. 
 
 In many portions of Marion and Harrison Counties, West Virginia, 
 the interval beginning 5 to 10 feet below the Waynesburg coal is occu- 
 pied by a hard, gray, massive sandstone, 20 to 35 feet thick. It is 
 finely exposed along the bed and bluffs of Ten Mile Creek, at and below 
 Browntown, Harrison County, West Virginia, and has been designated 
 from that locality. The deep, rocky cuts along the Baltimore and Ohio 
 liailroad, beginning 1 mile east of Mannington, Marion County, and 
 extending to the mouth of Mod’s Run, are all in this sandstone. It is 
 sometimes called the “ Gilboy ” sandstone, from a rocky cut of that 
 name near Mannington. This is nearly always a water-bearing stratum, 
 and the oil wells of Marion County have to be cased below this rock in 
 order to shut off the fresh water. 
 
 THE LITTLE WAYNESBURG COAL. 
 
 At many localities around the northern end of the Upper Coal Meas- 
 ure area a thin streak of coal or bituminous slate occurs at 25 to 40 
 feet below the Waynesburg coal, and it was termed the Little Waynes- 
 burg coal by Prof. Stevenson. It seldom exceeds 1 foot in thickness, 
 and is of no economic importance. It is usually separated from the 
 main coal above by shales and sandy beds, and should probably be 
 regarded as an offshoot from the Waynesburg coal proper. It is seldom 
 seen south from the Pennsylvania line, though it occurs along the Ohio 
 River at several places. 
 
 THE WAYNESBURG LIMESTONE. 
 
 Directly under the last described stratum there occurs a limestone 
 of very wide distribution. Its place is generally about 40 feet below 
 the Waynesburg coal, though sometimes it is less, and occasionally a 
 few feet more. It is usually of a dark gray color, and several of the 
 layers make excellent lime for agricultural and building purposes. The 
 thickness in Pennsylvania and northern West Virginia is seldom less 
 than 8 feet, and frequently double that, but south westward, toward the 
 Great Kanawha region, the limestone disappears entirely. 
 
 THE UNIONTOWN SANDSTONE. 
 
 At 60 to 75 feet below the top of the series there frequently occurs 
 a massive, gray sandstone whose horizon comes immediately above the 
 Unioutown coal; and hence, although the stratum in question is not 
 prominent at Uniontown, it has been designated from its relations to 
 the underlying coal. 
 
 The rock has occasionally been mistaken for the Waynesburg sand- 
 stone, which belongs nearly 100 feet above. It is well exposed at Bob- 
 
WHITE.] 
 
 THE UPPER COAL MEASURES. 
 
 59 l 
 
 town, Greene County, Pennsylvania, where it crowns the summit of the 
 hill overlooking Dunkard Greek as a bold cliff. 
 
 In the Georges Creek coal field a massive sandstone occurs 250 feet 
 above the Pittsburgh coal, and it was once referred by the writer to 
 the Uniontown horizon under the name of “ Westernport sandstone,” 
 but subsequent study seems to place it in the horizon of the Waynes- 
 burg sandstone. 
 
 THE UNIONTOWN COAL. 
 
 This bed underlies the Waynesburg coal by an interval of 80 to 100 
 feet, and is of economic importance only in Fayette and Washington 
 . Counties, Pennsylvania. It was named by Kogers from Uniontown, 
 Fayette County, where it is well exposed. The thickness seldom ex- 
 ceeds 3 feet, even in the region of its best development, and the coal 
 has never been used except for domestic purposes, since it is usually 
 neglected for the great Pittsburgh bed below. It often contains a 
 clay or slate parting near the center, 4 to G inches thick, and is rather 
 too rich in ash for a first-class fuel. 
 
 Southward from Fayette County, through Greene, Monongalia, Mar- 
 ion, and Harrison, this coal thins away to a bed of black slate mixed 
 with slaty coal that is often rich in fish remains and bivalve crusta- 
 ceans, which may be found in abundance near Davistown, Greene 
 County, Pennsylvania. 
 
 Along the Ohio Eiver at Wheeling, Bellaire, Clarington, and other 
 points, this bed is sometimes represented by a thin streak of black slate 
 or coal. In the Salisbury basin of Pennsylvania it is recognized by 
 Messrs. Platt, and is there over 3 feet thick, with slate near center. 
 
 THE UNIONTOWN LIMESTONE. 
 
 To the division of the u Great” Limestone which immediately under- 
 lies the last described coal bed, Dr. Stevenson gave the name Union- 
 town, since it seems to be fairly well separated from the great mass of 
 limy deposits below. This division is usually 10 to 15 feet thick, though 
 occasionally it surpasses these figures. The rock is frequently impure 
 and of a huffish color, being magnesian, and occasionally a good cement 
 rock, as at Uniontown, Pennsylvania. This is the only member of the 
 “ Great” Limestone which appears to be persistent from the Pennsyl- 
 vania line southward across West Virginia to the Big Kanawha River, 
 since an impure limestone only 2 to 5 feet thick occurs at this horizon 
 in the vicinity of Raymond City and other points in that region. 
 
 In the Salisbury basin this limestone occurs only 160 feet above the 
 Pittsburgh coal, and is 10 to 12 feet thick, according to Platt. 
 
 THE “ GREAT ” LIMESTONE. 
 
 This name, given by Rogers, is generally applied to all of the great 
 mass of lime deposits which intervene between the Uniontown and 
 Sewickley coals, though, as already stated, the name Uniontown is now 
 given to the uppermost division of the same. 
 
60 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65. 
 
 At many localities in Greene, Washington, Fayette, and Monongalia 
 Counties there are nearly 160 feet of limestones and limy shales at this 
 horizon, and the same beds hold their place, though with diminished 
 thickness, across to the Ohio Eiver at Wheeling. Westward and south- 
 ward, however, from Ohio and Marion Counties, these limestones disap- 
 pear very rapidly, so that at Clarksburg on the one hand, and west- * 
 ward through Ohio on the other, they have practically disappeared, 
 and in their stead we find shales, gray at first, but gradually getting 
 reddish toward the Little Kanawha Eiver and the western margin of 
 their outcrop in Ohio. On the Big Kanawha much red shale occurs at 
 this horizon. These limestones are of different qualities, some of the 
 layers being quite pure and forming good fluxes for iron, while others 
 are magnesian and make excellent hydraulic cements. 
 
 The only fossils ever seen in any of these limestone beds are fish re- 
 mains and minute ostracoids. 
 
 THE SEWICKLEY SANDSTONE. 
 
 At many localities where the u Great v Limestone is well developed 
 there are no other beds except limestones and shales in all of the inter- 
 val between the Uniontown and Sewickley coals, but in other regions 
 a sandstone frequently makes its appearance just above the Sewickley 
 coal. This has been called the Sewickley sandstone, and while it is 
 often flaggy, yet again it becomes massive, and even pebbly, varying 
 in thickness from 20 to 60 feet. Its massive character is well shown 
 along the Monongahela Eiver between Morgantown and Fairmont, in 
 the vicinity of the Big Falls. 
 
 THE SEWICKLEY COAL. 
 
 Directly under the Sewickley sandstone, or in its absence the u Great 79 
 Limestone, there comes the Sewickley coal, a bed which is widely per- 
 sistent, though the area where it is valuable is not so large. 
 
 The bed attains its maximum thickness and importance along the 
 Monongahela Eiver in Greene, Monongalia, and Marion Counties, beiug 
 there 5 to 6 feet thick, with only one slate parting of 2 to 3 inches near 
 the center. The coal is generally high in both ash and sulphur, but is 
 open-burning and makes a rather fair domestic fuel. 
 
 The following represents the general structure of this bed along the 
 Monongahela Eiver in Marion and Monongalia Counties : 
 
 Ft. in. 
 
 Coal 2 8j 
 
 Slate 0 2} 5' 6" 
 
 Coal 2 8 j 
 
 Followed down the Monongahela Eiver, the bed retains about the 
 same structure as far as the mouth of Whitely Creek, Greene County, 
 Pennsylvania, when the slate partings thicken up, and new ones come 
 in and dissipate the coal in several thin layers through 25 feet of rock 
 
geological survey Bulletin no. 65 Rl. Vii 
 
 UPPER COAL MEASURES AT POINT PLEASANT, WEST VIRGINIA, SHOWING RUGGED CHARACTER OF THE T_ . _GRAPHY. 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
WHITE.] 
 
 THE UPPER COAL MEASURES. 
 
 61 
 
 material, and from thence on down that river it is of no importance. 
 But followed in the other direction, up the Monongahela, this bed holds 
 a thickness of 5 to 6 feet through Marion County until the Harrison 
 County line is approached, when it again splits up into three or four di- 
 visions separated by several feet of shales and slates, and when Clarks- 
 burg is reached there remains only 1 foot of coal at this horizon (Sec- 
 tion 18), which soon disappears entirely toward the southwest. 
 
 From the Monongahela region this coal dips down westward under 
 the great mantle of Permo-Carboniferous beds, and when it reappears 
 on the Ohio River, in the vicinity of Wheeling (Section 19), Bellaire 
 (Section 20), and Pipe Creek (Section 22), we find it split up again into 
 three or four layers, and the separating slates several feet thick, thus 
 giving the whole bed a thickness of 20 to 30 feet, with the main coal 
 layer at the top. 
 
 This uppermost division of the Sewickley is separated from the Pitts- 
 burgh below by an interval of 80 to 100 feet, and attains considerable 
 importance in the counties of Belmont, Harrison, Guernsey, Monroe, 
 Morgan, Muskingum, Noble, etc., and has there been mined under a 
 variety of names, among which are “ Upper Barnesville,” “ Upper Bel- 
 laire,” “ Cumberland,” u Meigs Creek,” and several others. Prof. Orton, 
 while intimating its identity with the Sewickley of Pennsylvania (Vol. 
 Y, page 1059, Ohio Geology), prefers to call it by the name of Meigs 
 Creek, from a stream in Morgan County along which it is well devel- 
 oped. 
 
 Throughout much of this Ohio region the coal is 3 to 4J feet thick, 
 and nearly always has a clay or bony streak near its center. It also 
 frequently has a rider coal in the roof, and the entire bed is rather rich 
 in ash and sulphur, according to Orton. 
 
 In Fayette County, Pennsylvania, the Sewickley coal has a thickness 
 of 4 to 5 feet through several townships, according to Stevenson, but 
 northward through Westmoreland it thins down and is unimportant. 
 It is scarcely known in the Ligonier basin, but in that of Salisbury is 
 2 feet thick and 90 feet above the Pittsburgh. 
 
 In the Georges Creek basin of Maryland and West Virginia the bed 
 is 5 to 7 feet thick, 90 to 115 feet above the Pittsburgh, and an excellent 
 coal for steam purposes. 
 
 The oil-borings across Monongalia and Marion Counties reveal this 
 coal present in good thickness 10 to 15 miles west from the Mononga- 
 hela River, and 100 to 110* feet above the Pittsburgh coal. The oil 
 drillers usually call it the “Mapletown” coal, from a locality in Greene 
 County where it is mined. 
 
 THE SEWICKLEY LIMESTONE. 
 
 The interval between the Sewickley coal and the one next below is 
 •often occupied largely by limestone, especially in Greene, Fayette, 
 Washington, Monongalia, and Marion Counties, and to the one which 
 
62 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 BULL. 65. 
 
 comes next below the coal Messrs. Platt have given the name Be- 
 wick ley. It has also been termed the Fishpot Limestone by Ste- 
 venson, from a small stream in Washington County. I have deemed it 
 preferable to apply the name Sewickley to the whole limestone group 
 which lies between the Sewickley and Redstone coal beds. This inter- 
 val is 40 to 60 feet thick and sometimes contains two beds of sandstone 
 intercalated with the limestones. Along the Monongahela River iu. 
 Greene, Monongalia, and Marion Counties, these limestones are well 
 developed, and many of the layers furnish excellent lime for mortar and 
 agricultural uses, while near the base of the group occur some excellent 
 limestone flags at Laurel Point, Monongalia County. 
 
 The only fossils ever noted in these beds are minute fresh- water types. 
 
 These limestones disappear southward from Harrison Qounty, West 
 Virginia, there being only 9 feet of them in the Clarksburg section, and 
 none on the Little and Big Kanawha Rivers. The same thing takes 
 place in Ohio, westward from Washington County, the interval being- 
 occupied by shales and sandstones. 
 
 In Pennsylvania this Sewickley limestone holds a prominent place 
 eastward from Washington and Greene, through Fayette, Westmore- 
 land, and Somerset Counties. 
 
 TftE REDSTONE COAL. 
 
 In Fayette County, Pennsylvania, a small coal was found cropping 
 out along Redstone Creek, at an interval of 40 to 45 feet above the 
 Pittsburgh, and this was named from that stream by the geologists 
 of the First Pennsylvania Geological Survey. 
 
 Monongalia is the only county in West Virginia where this bed is 
 workable, it being there, on Scott’s and Robinson’s Runs, 4 to 5 feet 
 thick and of fair quality, though having rather too much sulphur and 
 ash for manufacturing purposes. It is also workable in several town- 
 ships of Fayette and Westmoreland, being 3 to 4 feet thick. In the 
 Salisbury basin of Somerset County, Messrs. Platt identify the Red- 
 stone coal as a slaty bed, 4 feet thick, at 45 feet above the Pittsburgh. 
 It has not been reliably reported from the Georges Creek field unless 
 it be represented by one of the rider layers in the roof of the Pitts- 
 burgh bed. 
 
 In the vicinity of Wheeling, Bellaire, and other points on the Ohio 
 River, this bed is only a few inches thick, never becoming workable 
 anywhere in Ohio. 
 
 Through central West Virginia, beyond the Little Kanawha, its pres- 
 ence is unknown except by a bed of black slate which is occasionally 
 seen at this horizon. 
 
 THE REDSTONE LIMESTONE. 
 
 At many localities along the Monongahela River in Harrison, Marion, 
 Monongalia, Greene, Washington, Fayette, and Westmoreland Coun- 
 ties, there occurs a bed of limestone often 10 to 20 feet thick, and im- 
 
WHITE. ] 
 
 THE UPPER COAL MEASURES. 
 
 63 
 
 mediately underlying the Redstone coal. From this latter fact it was 
 termed the Redstone limestone by Messrs. Platt, who find the same 
 bed in Somerset County, 40 to 45 feet above the Pittsburgh coal. It 
 often contains several layers, which make fairly good lime for many 
 purposes, and is occasionally used for flux in iron furnaces. 
 
 This limestone is also in great force in the vicinity of Wheeling, Bel- 
 laire, and vicinity, where it occupies nearly the entire interval between 
 the Redstone and Pittsburgh coals, and is extensively quarried as a 
 flux for the furnaces there. 
 
 It, like all the other limestones, disappears southwestward through 
 West Virginia, and is not known beyond the Little Kanawha River. 
 
 THE PITTSBURGH SANDSTONE. 
 
 Very frequently, and especially when the Redstone limestone is well 
 developed, there is nothing but shales intervening between it and the 
 Pittsburgh coal, but when the limestone is absent, or but poorly repre- 
 sented, there is often present a coarse, massive sandstone immediately 
 above the Pittsburgh coal, and to this Mr. H. D. Rogers long ago gave 
 the name of Pittsburgh sandstone. It varies in thickness from 25 up 
 to 70 feet, and is usually coarse, friable, and often pebbly. Good build- 
 ing stone has never been obtained from it, since it yields so readily to 
 atmospheric agencies. 
 
 This rock is especially massive in the vicinity of Hartford City, 
 Pomeroy, and other contiguous regions, and the same may be said of 
 the eastern line of its outcrop from Pennsylvania clear across West 
 Virginia to the Kentucky border. 
 
 In the Georges Creek, Salisbury, and Ligonier basins, however, this 
 rock makes but little show in the topography, its place being occupied 
 by soft shales. 
 
 THE PITTSBURGH COAL. 
 
 The last and lowest member of the Upper Coal Measures is the cele- 
 brated Pittsburgh bed, the most important mineral deposit of the Ap- 
 palachian field. 
 
 It was formerly thought that this coal bed was entirely persistent ; 
 that wherever its horizon was to be found, there the coal might be 
 expected with absolute certainty. This generalization, however, was 
 founded on data obtained only from the northern half of its area. In 
 Pennsylvania, for instance, no area has yet been discovered where, at 
 the proper geological horizon for this bed, it does not exist. Even in 
 central Greene, at a depth of 1,500 feet below the Permo-Carboniferous 
 summits, the drill of the petroleum seeker invariably finds this coal 
 bed, while the isolated peak of Round Top, in the Broad Top coal basin 
 of Bedford County, 50 miles distant from any other outcrop of the coal, 
 likewise contains it. But when we pass southwestward across the West 
 Virginia and Ohio coal field, Pennsylvania conditions of course continue 
 
64 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65 . 
 
 for many miles, but ultimately there comes a change, and when we look 
 for the Pittsburgh bed it is gone, or so reduced in thickness that the 
 geologist can only recognize it by its associated rocks. The region of 
 country covered by this barren area is quite extensive, and seems to 
 be rudely coincident with the line of the Volcano or Burning Springs 
 anticlinal of West Virginia. 
 
 The following counties in that State have the coal but poorly devel- 
 oped or wanting at the horizon where it belongs : Calhoun, Boane, 
 Wirt, Kitchie, Pleasants, and Wood. This belt projected northward 
 through Ohio takes in the counties of Washington, Noble, and Mor- 
 gan, in all of which the coal is thin or wanting altogether. Thus it 
 happens that over a belt of country 30 to 50 miles wide, and running 
 nearly north and south across the Appalachian coal field, the spread 
 of this bed, so even and persistent at the north, is here irregular, inter- 
 rupted, and wanting. West from this belt the coal comes in again and 
 is fairly regular in parts of Kanawha, Putnam, and Mason Counties, 
 east from the Big Kanawha ; but west from that stream the bed is thin, 
 patchy, and of little importance through Cabell and Wayne, til bit dis- 
 appears from the center of the great Appalachian trough in the hilltops 
 overlooking the Big Sandy River. 
 
 In Ohio, also, a considerable area of this coal comes in west from 
 the barren belt, and extends ‘through Meigs and Athens Counties with 
 fairly good thickness, but westward from them, in Gallia, the coal is 
 again thin and uncertain. 
 
 The foregoing sections, Nos. 11 to 32 inclusive, show in a general 
 way the detailed structure of the Pittsburgh coal, so that oi * a few 
 others need be given in this connection to exhibit its structure iu 
 every important region of its widely extended area. 
 
 As will be seen from these sections, the coal is nearly always sepa- 
 rated into two well defined portions (the roof and the main bench) by 
 a layer of clay, and there are often several divisions of the rot f, as also 
 of the main bench. The layers of coal in the roof are usually not more 
 than 1 to 1J feet thick, and separated by shales of about the same 
 thickness, while the divisions of slate in the main bench are mere knife 
 edges, seldom exceeding an inch in thickness and generally not more 
 than half that amount. 
 
 Along the Monongahela River, two of these slates are especially con- 
 stant, since they come about 2J to 3 feet above the bottom of the bed 
 and are 4 to 6 inches apart. They are usually known as the “ bearing 
 in” slates, and are seldom more than one-lialf inch thick. Then 1 to 14 
 feet below these there is generally another thin parting of slate which 
 runs through the bed with great persistency, dividing the lower portion 
 into two layers known by the miners as the “ brick” coal, and “bot- 
 tom ” coal. Of course there are other partings which occasionally make 
 their appearance in the bed at some localities, but they are irregular 
 and not persistent. 
 
THE PITTSBURG COAL OUTCROP NEAR CONNELLSVILLE, PENNSYLVANIA, SHOWING COLUMNAR STRUCTURE OF TYPICAL COKING COAL. 
 
TKE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
WHITE. J 
 
 SECTION ON FAIRFAX KNOB, W. VA. 
 
 65 
 
 Section at Newburg , West Virginia.— The summits around Newburg, 
 Preston County, West Virginia, catch small areas of this bed in the 
 syncline between the Chestnut Eidge and Laurel Hill anticlinals, and 
 the coal has there the following structure : 
 
 Ft. in. 
 
 Pittsburgh sandstone 
 
 Slaty coal 0 
 
 Shale 0 
 
 Coal 0 
 
 Shale and fire clay 2 
 
 Coal 9 
 
 Slate 0 
 
 Coal, slaty 1 
 
 9! Ft - 
 » 4 
 0.1 
 0\ 
 
 3^10 
 
 6J 
 
 in. 
 
 31 
 
 Ft. 
 
 15 
 
 Section at Copeman’s Knob , West Virginia. — In the next trough east of 
 the Laural Hill anticlinal, a small isolated area of the Pittsburgh coal 
 is caught in Copeman’s Knob, which overlooks Cheat Eiver at the foot 
 of Briery Mountain, near Albrightsville, Preston County, West Vir- 
 ginia, and there the coal shows this structure : 
 
 f Shales 
 
 I Coal 
 
 j Slate 
 
 Roof. Coal, slaty 
 
 j Slate 
 
 j Coal 
 
 I Clay 
 
 Main coal, partings not visible 
 
 Ft. iu. 
 
 oi 
 
 « 
 
 4 ! Ft. 
 
 2> n 
 
 6 I 
 
 6j 
 
 j Ft. 
 V 19 
 
 10 J 
 
 Section 32 gives the structure of this coal still farther eastward in 
 the Georges Creek basin, and it, when compared with the Albright, 
 Newburg, and Fairmont (Sec. 17) structures, shows a gradual eastward 
 thickening of the bed from 7 feet on the Monongahela to 20 at many 
 points in the Georges Creek field. 
 
 Section at Fairfax Knob , Tucker County , West Virginia. — Near the 
 southern end of the Georges Creek basin, at the head of the North Po- 
 tomac Eiver, a small area of the Pittsburgh bed is caught in the sum- 
 mit of Fairfax Knob, 3,250 feet above tide, and 20 miles distant from 
 any other outcrop of the coal. The main portion of the bed is here 
 split into three portions, separated by several feet of shales, from the 
 thickening up of the parting slates, as follows : 
 
 Ft. in. Ft. 
 
 ( Shales.. 
 Roof . ) Coal — 
 ( Shale... 
 
 
 2 
 
 0 l 
 
 
 6 
 
 ol 
 
 Coal, “breast”. 
 
 , Coal 
 
 ) Slate 
 
 8' 2" \ 
 
 O' 2“ V 9 
 
 V 2" ; 
 
 5' 0“ \ 
 
 4' 0" >16 
 
 v o #/ S 
 
 4 
 
 6 
 
 Shales 
 
 Limestone 
 
 ( Coal 
 
 o l 
 
 Shales 
 
 Coal, “brick” .. 
 
 
 < 
 
 (I 
 
 Fireclay and shales 
 
 18 
 
 0 
 
 Coal, “bottom,” 
 
 slaty 
 
 7 
 
 OJ 
 
 Bull. G5 5 
 
66 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [HULL. 65 . 
 
 As will be seen from the above, it would appear that the three main 
 divisions ot the Pittsburgh bed, viz, “ breast,” u brick,” and “ bottom,” 
 are here separated by shales, 1G and 18 feet thick respectively, instead 
 of mere partings of a fraction of an inch, as on the Monongahela and 
 elsewhere, thus spreading the 21 feet of coal through an interval of 55 
 feet. It is also worthy of note that although the partings have here 
 Increased so wonderfully, yet the total thickness of coal remains the 
 same as in the central part of the Georges Creek Basin, 
 
 In the vicinity of Glenville, on the Little Kanawha Kiver, this coal 
 is 4J to 5 feet thick, with a bony streak 16 inches below the top of the 
 bed. 
 
 The structure on the Big Kanawha is given in Section 31. 
 
 Section at Huntington , Cabell County , West Virginia . — In the summits 
 of the hills south of Huntington, Cabell County, West Virginia, this 
 coal displays the following structure : 
 
 Ft. 
 
 Coal 0 
 
 Clay 0 
 
 Coal 3 
 
 Slaty coal 0 
 
 in. 
 
 6^1 
 
 j Ft. 
 
 6 I 
 
 2J 
 
 The farthest point to the southwest that this bed has ever been seen 
 is in the summit of a hill overlooking the Big Sandy Kiver, 10 miles 
 above its mouth, where a small patch is caught in the center of the 
 Appalachian trough, which, rising to the southwest, carries the coal 
 above the highest hills on the Kentucky side of the Big Sandy. The 
 coal is here 3 feet 2 inches thick and single bedded, or with only faint 
 partings. 
 
 Section at Pomeroy , Meigs County , Ohio. — At Pomeroy, Ohio, the 
 Pittsburgh coal shows thus, according to Prof. E. Lovejoy. Ohio Geo- 
 logical Survey, Vol. VI, page 636: 
 
 In. 
 
 Coal 8-14 "j 
 
 Horn coal 3 j Ft. in. 
 
 Coal . ..42-47 > 5 10 
 
 Clay . 4 | 
 
 Coal 7 J 
 
 Section on Shade Creek , Ohio. — In the Shade Creek coal field of Meigs 
 and Athens Counties, Ohio, Prof. Lovejoy finds a well developed rider 
 coal 12 to 20 feet above the main bed, and often mined separately from 
 it. The two have the following structure : 
 
 Ft. in. 
 
 Coal 0 6^ Ft. in. 
 
 Slate- 0 4 > 2 8 
 
 Coal 1 10 j 
 
 Shales 12-20 
 
 Coal 0 9 
 
 Slate, streak 0 0 
 
 Coal 2 6 
 
 Slate, streak 0 0 
 
 4 3 
 
. 
 
 white.] SECTION IN BELMONT COUNTY, OHIO 67 
 
 Section on Federal Creek , Ohio. — In the Federal Creek field of Athens 
 and Morgan Counties, Ohio, the coal shows as follows (Lovejoy), op. 
 cit., p. 648, Heyburn Brothers & Co.’s mine, Berne Township, Athens 
 County : 
 
 /. Ft. in. 
 
 Coal 1 10^ 
 
 Slate, streak 0 0 
 
 Coal 2 4 
 
 Slate 0 7 I Ft. 
 
 Coal 0 3 > 10 
 
 Clay 1 0 
 
 Coal. 1 0 
 
 Slate, streak 0 0 
 
 Coal 3 0, 
 
 Section at Berry's mine , Ohio. — Berry’s mine, in Homer Township, 
 Morgan County (op. cit. page 650), gives the following : 
 
 Ft. in. 
 
 Coal : 0 11 
 
 Slate, streak 0 0 I 
 
 Coal 3 5 f 5 4 
 
 Clay 1 0 j 
 
 Coal 0 4*1 
 
 Slate, streak * 0 0 
 
 Coal 0 7 \ 
 
 Slate, streak 0 0 ► 3 7* 
 
 Coal 1 10 
 
 Slate, streak 0 0 
 
 Coal 0 9f 
 
 • 
 
 The clay stratum in these and other mines appears to correspond to 
 the main clay parting which always separates the roof coals of the 
 Pittsburgh bed from the main bench along the Monongahela, and the 
 12 to 20 feet of shales which separate the two coal beds in the Shade 
 Creek field would appear to belong at the same horizon. 
 
 East from the barren area of the Pittsburgh coal of Morgan, Noble, 
 and Washington Counties, Ohio, it comes in again with a fine develop- 
 ment in Belmont, Harrison, and Jefferson. 
 
 Section in Belmont County , Ohio. — The following section from Ohio 
 Geology, Yol. YI, page 621, exhibits the structure in the southern por- 
 tion of Belmont County, Washington Township, as given by Prof. 
 Brown : 
 
 
 Ft. 
 
 in. Ft. 
 
 iu. 
 
 Coal 
 
 
 ° l 1 
 
 
 Clay 
 
 0 
 
 10-12 ( 1 
 
 11 
 
 Coal 
 
 2 
 
 9 1 
 
 
 Slate 
 
 0 
 
 01 | 
 
 
 Coal 
 
 2 
 
 0 )> 6 
 
 0 
 
 Slate 
 
 0 
 
 oi| 
 
 
 Coal 
 
 1 
 
 2 J 
 
 
68 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section at Bellaire, Belmont County , Ohio. — In Bellaire the following 
 is shown at Heatlierington’s mine: 
 
 Ft. in. 
 1 0 
 
 I 
 
 | Ft. in. 
 } 3 2 
 
 J 
 
 Coal 
 
 Black slate 0 4 
 
 Coal •- 1 0 
 
 Clay 0 10 
 
 Coal 2 6 
 
 Slate 0 0 
 
 Coal 0 5 
 
 Slate 0 0 
 
 Coal 1 9 
 
 Black slate, pyritous 0 01 
 
 Coal 1 0 
 
 Hard, slaty coal 0 4 
 
 Section in Jefferson County , Ohio . — In Warren Township, Jefferson 
 County, Ohio, this coal has the following structure (Brown, Ohio Geol- 
 ogy, Vol. VI, page 603) : 
 
 6 0 * 
 
 Roof coal ' 
 
 Clay 
 
 Coal 
 
 Clay parting 
 
 Coal 
 
 Black slate v 0 
 
 Coal 1 
 
 Parting 
 
 Coal 1 
 
 Ft. 
 
 2 
 
 0 
 
 2 
 
 0 
 
 0 
 
 3 
 
 4 
 2 
 2 
 2 
 £ 
 
 3 
 
 2J 
 
 Ft. in. 
 2 7 
 
 > 4 11 
 
 Section in Harrison County , Ohio. — In German Township, Harrison 
 County, Ohio, Stevenson reports the Pittsburgh coal as follows (Ohio 
 Geological Survey, Vol. Ill, p. 212): 
 
 Ft. in. 
 
 Roof coal, not exposed 0 
 
 Coal...- 
 Parting . 
 
 Coal 
 
 Parting . 
 Coal.... 
 Parting . 
 Coal 
 
 0 
 
 9 1 
 Oil 
 
 6 | Ft. in. 
 li} 4 9£ 
 2 
 0£ 
 
 2 j 
 
 Section at Columbia mine , Westmoreland County , Pennsylvania. — As a 
 typical section of this coal on the Monongahela River with reference to 
 the structure of the main bench and roof, we may take that found at the 
 Columbia mine, near Webster and 361 miles above Pittsburgh, as given 
 by Mr. J. Sutton Wall (K 4 , Pennsylvania Geological Survey*, p. 50) : 
 
 Ft in. 
 
 4 3 
 
 Roof coals, in seven divisions 
 
 Ft. 
 
 3 
 
 in. 
 
 ° l 
 
 Over-clay 
 
 0 
 
 6 i 
 
 “ Breast 7 ’ coal 
 
 3 
 
 8 ' 
 
 Parting 
 
 0 
 
 0J 
 
 “Bearing in” coal 
 
 0 
 
 3 
 
 Parting 
 
 0 
 
 0£ ► 
 
 “ Brick ” coal 
 
 1 
 
 2 
 
 Parting 
 
 0 
 
 01 
 
 “Bottom ” coal 
 
 1 
 
 4 J 
 
WHITE] 
 
 FOSSILS OF THE UPPER COAL MEASURES. 
 
 69 
 
 A careful comparison of the structure of this famous bed at a great 
 many points very widely separated exhibits such a striking resemblance 
 to that just given above that we can scarcely attribute it to chance, 
 but must find the explanation in the prevalence of nearly uniform con- 
 ditions over the immense area covered by the Pittsburgh marsh. 
 
 The great excellence of this coal for steam and domestic purposes, 
 and also for the manufacture of gas and coke, combine to render it the 
 most valuable bed of coal in the entire Appalachian field. 
 
 Page plate 6 gives a view of this bed at Conoellsville, the center of 
 the coke-making industry, and in this the peculiar columnar structure 
 of a typical coking coal is fairly shown. 
 
 It was formerly believed that this bed would not make first-class 
 coke over any large area outside of the Oonuellsville basin, but recent 
 developments along the Monongahela River in Marion and Monongalia 
 Counties, West Virginia, have proved this belief erroneous, since it is 
 there successfully coked on a large scale. 
 
 By crushing and washing, where there is too much sulphur present, 
 there is no reason why this bed will not make coke equal to that of the 
 Connellsville, throughout all of the region south and west from the 
 latter. 
 
 The roof coals of this bed are never mined ; not because they do not 
 furnish good fuel, but because they are always interstratified with 
 shale, which renders the mining difficult. These roof layers often 
 amount to 3 or 4 feet of good coal, and thus this large quantity of fuel 
 is continually wasted, though the time will doubtless come in the dis- 
 tant future when the Pittsburgh bed will be mined over again for the 
 coal now neglected in its roof and bottom. 
 
 FOSSILS OF THE UPPER COAL MEASURES. 
 
 The flora of the Pittsburgh roof shales as well as of the entire Upper 
 Coal Measures is very meager, and only a few of the very common 
 types, like Neuropteris hirsuta , N. flexuosa , and Pecopteris arborescent, 
 are usually found, while the fauna of the whole group, so far as known 
 at present, seems to be restricted to fresh water types. 
 
CHAPTER IV. 
 
 THE BARREN MEASURES, OR ELK RIVER SERIES. 
 
 THICKNESS, CHARACTER, AND EXTENT. 
 
 Below the Pittsburgh bed we descend into a very natural group of 
 rocks (No. XIV) which was long ago clearly recognized by the Rogers 
 brothers in both Pennsylvania and Virginia. The group as defined by 
 them extended from the base of the Pittsburgh coal down to the top of 
 the Mahoning sandstone, and was called the Lower Barren Measures ; 
 but subsequent investigation seems to render it more desirable to ex- 
 tend the group downward so «as to include the Mahoning sandstone. 
 This brings the group within the definite limits of two important and 
 very persistent coal beds, the Pittsburgh above and the Upper Free- 
 port below; and hence, for purposes of comparison, study, and all the 
 uses which classification subserves, is more desirable than the old 
 system, since the top of the Mahoning sandstone is too variable a 
 quantity for the limit of any group. 
 
 I have already indicated in a previous chapter that a larger view of 
 the Carboniferous Measures, which overlooks details invaluable for 
 classification to the working geologist, would run a line through the 
 middle of the Barren Measures, and call everything above it, to the 
 top of the Dunkard Creek series, Upper Carboniferous; that below it, 
 to the base of the Pottsville conglomerate, Middle Carboniferous, and 
 the rest down to the Catskill, Lower Carboniferous. Such a classifica- 
 tion of the Appalachian Carboniferous may be useful for comparison 
 with the Carboniferous system in other regions and countries, but it is 
 too general for the practical geologist, and can never supplant that 
 which has stood the test of long and continuous use. Hence we deem 
 it best to retain the limits of the Barren Measures intact, with the 
 slight modification just suggested, and already long in use by the 
 Second Geological Survey of Pennsylvania. 
 
 I have adopted the name Elk River series as a geographical designa- 
 tion for these beds, since they are very finely exposed along that stream 
 between its mouth at Charleston, West Virginia, and Braxton Court- 
 House, or Sutton, nearly 100 miles above. 
 
 70 
 
WHITE.] 
 
 THE ELK RIVER SERIES. 
 
 71 
 
 This series, as thus limited above and below by important coal beds, 
 consists of two very different members; an upper one composed largely 
 of shales, therefore soft, easily eroded, and always making rounded 
 hills and rolling topography ; the other, or lower, composed largely of 
 massive sandstones which resist erosion and thus form steep cliffs, deep 
 gorges, rugged topography, and wild scenery generally. 
 
 These sand rocks form a coping to the Lower Coal Measure hills, and 
 cap the summits long after the soft beds above have disappeared. 
 
 The soil formed by the soft member, while rather thin and not to be 
 compared in fertility to that of the Upper Coal Measures, yet with care 
 and a liberal use of lime yields excellent crops and always makes 
 good grazing lands. But the lower portion, being almost destitute of 
 lime, and containing so much sand, forms a very poor soil, on which 
 only the scantiest crops can be grown. 
 
 The upper portion always contains a large percentage of red and 
 marly shales, which make a broad band of red soil from Pennsylvania 
 clear through central West Virginia, to and beyond the Kentucky line 
 on the one hand, and thence circling around through eastern Kentucky 
 and southern Ohio, back to Pennsylvania again on the other. These red 
 clays are the fruitful source of landslides, bad roads, and many other 
 troubles. They cave easily in drill holes, and thus give endless annoy- 
 ance and expense to oil and gas drillers. Their tendency to slide 
 causes much expense in cleaning out railroad cuttings, so that a proper 
 knowledge of their character by engineers would lead to economy of 
 money in building and maintaining both railroads and wagon roads. 
 
 The coal beds of this series are, with one or two exceptions, noted 
 for their variableness and uncertainty. They may be in fair develop- 
 ment on one farm, and absent entirely on the adjoining one. They are 
 also usually rich in ash and poor in carbon, and although they are 
 patchy in their distribution, yet the main beds appear to maintain the 
 same horizons in the stratigraphy, and can thus be identified with 
 reasonable certainty over wide areas. The sandstones found within 
 the limits of this group are of more economic importance than the coal 
 beds, since the former nearly always furnish most excellent building 
 stone, while the latter are commercially valuable only over limited 
 areas. Iron ore in valuable quantity exists locally at several horizons 
 in the Barrens, and these will be referred to hereafter in detail. 
 
 The limestones of this series, like the coals, are generally thin and 
 impure, so that they are of more importance in determining the strati- 
 graphy than for economic purposes. 
 
 The entire thickness of the group varies much in different portions 
 of the Appalachian field, reaching a maximum of 800 feet in the vicinity 
 of Charleston, West Virginia, while along the northwestern outcrop of 
 the beds in Ohio the minimum is not much above 300 feet. 
 
 In Pennsylvania and northern West Virginia the average is about 
 600 feet, but it sometimes runs up to 650 and down to 550. 
 
72 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BUM.. 65. 
 
 The following sections, taken in the several portions of the Appa- 
 lachian held, will serve to illustrate both the changing thickness of the 
 series and the variable nature of the individual beds. 
 
 Section in the Pittsburgh region . — We shall begin the 
 list at Pittsburgh, where the upper half of the Bar- 
 rens is finely exposed, and the numerous carefully 
 kept records of drill holes have revealed the constitu- 
 tion of the lower half, so that by uniting the two we 
 get the following (Fig. 33) : 
 
 7t>* 
 
 ilil 
 
 iSi 
 
 mm 
 
 
 In Pittsburgh region. 
 
 [See map, I m.] 
 
 Pittsburgh coal 
 
 Concealed 
 
 Limestone 
 
 Shales, variegated 
 
 Limestone 
 
 Rod shale 
 
 Concealed 
 
 Sandstone, Morgantown 
 
 Coal, Elk Lick 
 
 Shales, variegated 
 
 Coal 
 
 Limestone 
 
 Shales, variegated 
 
 Limestone, crinoidal * 
 
 Coal, crinoidal 
 
 Red and variegated shale 
 
 Sandy shales and shaly sandstone 
 
 , Coal, Bakerstown 
 
 Shales and sandstone 
 
 Limestone, Upper Cambridge 
 
 Sandstone, massive 
 
 Limestone, Lower Cambridge 
 
 Shales 
 
 Coal, Masontown 
 
 Shales 
 
 Sandstone, Mahoning 
 
 Upper Freeport coal. 
 
 Total 
 
 Ft. 
 
 Ft. 
 
 227 
 
 90 
 
 114 
 
 2 
 
 50 
 
 1 
 
 10 
 
 1 
 
 20 
 
 100 
 
 618 
 
 Fio. 33.— Section in 
 the Pittsburgh region. 
 
WHITE. ] 
 
 THE BARREN MEASURES. 
 
 73 
 
 Section at Sewickley , Pennsylvania.— At Sewickley, Pennsylvania, a 
 diamond-drill hole was put down by Mr. Cochran Fleming as a test 
 for coal. The cores were carefully preserved, and 
 from them I obtained a very accurate section of t lie 
 lower portion of the Barrens, which, combined with 
 the good surface exposures around Sewickley, gives 
 the following structure (Fig. 34) for this series in 
 that region : 
 
 205* 
 
 
 ■I 
 
 ao' 
 
 4 tf 
 
 WMm 38 ' 5 " 
 
 ivXvXvV’/. 
 
 I35’> 
 
 Sewickley, Alleghany County, Pennsylvania. 
 
 [See map, HI.] 
 
 Ft. in. 
 
 1. Pittsburgh coal 
 
 2. Shales, sandstones, and concealed 180 
 
 3. Sandstone, Morgantown, massive 25 
 
 4. Coal, Elk Lick 
 
 5. Shales and sandstone 
 
 6. Limestone, crinoidal 
 
 7. Coal, crinoidal 1 
 
 8. Red shales and sandy beds 110 
 
 9. Limestone, gray, Upper Cambridge 2 
 
 10. Shales and concealed 40 
 
 11. Sandy shale 32 
 
 12. Dark slate 11 
 
 13. Limestone, dark, Lower Cambridge 
 
 14. Dark shales 
 
 15. Coal, Mason town 
 
 16. Sandstone, micaceous, gray 13 
 
 17. Fire clay, sandy 0 
 
 18. Sandstone, light gray 22 
 
 19. Shale, dark gray 8 
 
 20. Sandstone, gray 0 
 
 21. Shale, sandy 6 
 
 22. Shale, blue 6 
 
 23. Sandstone 0 
 
 24. Slate, gray 3 
 
 25. Fire clay, variegated at base, impure 25 
 
 26. Sandstone, gray, micaceous 38 
 
 27. Shales, sandy, blue 8 
 
 28. Sandstone, light gray 8 
 
 [ 29. Upper Freeport coal. 
 
 Total . 
 
 Ft. 
 
 205 
 
 6 ) 
 
 196 
 
 . 135 7 
 
 sy* ' 
 
 634 
 
 Fig. 34. — Section at 
 Sewickley, Pa. 
 
 The interval No. 2 in this section was estimated, 
 since the Pittsburgh coal is not found in the imme- 
 diate vicinity of Sewickley, the highest stratum 
 remaining there being the Morgantown sandstone, 
 No. 3. 
 
74 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section on Dunbar Creek , Pennsylvania . — Eastward from the Pittsburgh 
 region, we have a line of measurements of the Barren series which ex- 
 tend across the Alleghanies. The first one is in the 
 adjoining county of Fayette, at the foot of Chest- 
 nut Bidge, made by Prof. Stevenson and published 
 in his Beport KK, page 182. It is as follows (Fig. 
 35): 
 
 Dunbar Creek , Fayette County , Pennsylvania. 
 
 
 42' 
 
 65* 
 
 35 ' 
 
 [See map, K n.] 
 
 Fig. 35.— Section on 
 Dunbar Creek, Pa. 
 
 1. Coal, Pittsburgh 
 
 2. Concealed... , 15 
 
 3. Sandstone 10 
 
 4. Coal, Little Pittsburgh 0 
 
 5. Clay 3 
 
 6. Limestone and shale 20 
 
 7. Sandstone, Connellsville 60 
 
 8. Shales 50 
 
 9. Limestone.! 5 
 
 10. Shale 5 
 
 11. Sandstone, Morgantown 55 
 
 12. Shale, sandy* 12 
 
 13. Coal, Elk Lick 
 
 14. Shale 12 
 
 15. Concealed 12 
 
 16. Shale, variegated 35 
 
 17. Coal, clay, crinoidal 
 
 18. Shales, brown 10 
 
 19. Sandstone 28 
 
 20. Shale J 45 
 
 21. Coal, Bakerstown 2 
 
 22. Shale 63 
 
 23. Limestone, Lower Cambridge 
 
 24. Shale 7 
 
 25. Sandstone, argillaceous 10 
 
 26. Concealed 25 
 
 27. Coal, Masontown 
 
 28. Clay 30 
 
 29. Sandstone, Upper Mahoning 35 
 
 30. Coal, Mahoning 
 
 31. Fire clay 
 
 32. Sandstone, Lower Mahoning 
 
 33. Coal, Upper ‘Freeport. 
 
 Total 
 
 Ft. in. Ft. m. 
 
 235 
 
 148 
 
 598 6 
 
 The identification of the Lower Cambridge limestone in the above 
 section is open to question, but the probabilities are in favor of the one 
 given. 
 
WHITE.] 
 
 THE BARREN MEASURES, 
 
 75 
 
 Section at Ligonier , Pennsylvania . — Eastward from the last locality, 
 and between Chestnut Ridge and Laurel Hill, the following section 
 (Fig. 36) of these beds was measured at Ligonier, 
 Westmoreland County, Pennsylvania, by Prof. Stev- 
 enson, as given in Report KKK, page 129 : 
 
 Ligonier , Westmoreland County, Pennsylvania . 
 
 L===s§r==2o 
 
 153 ? 
 
 [See map, J p.] 
 
 Ft. in. 
 
 1. Pittsburgh coal 
 
 2. Concealed 60 
 
 3. Coal, Little Pittsburgh 1 6 
 
 4. Limestone 8 
 
 5. Concealed 27 
 
 6. Shale, variegated 43 
 
 7. Coal, Little Clarksburg . 
 
 8. Shale 10 
 
 9. Concealed 10 
 
 10. Sandstone, Morgantown 115 
 
 11. Shale, olive .* 18 
 
 12. Coal, Elk Lick 
 
 13. Shale 
 
 14. Limestone, green, fossiliferous 
 
 15. Shale 20 
 
 16. Sandstone 5 
 
 17. Clay 8 
 
 18. Limestone, ferruginous 2 
 
 19. Shale 10 
 
 20. Sandstone 25 
 
 21. Concealed 100 
 
 22. Shale 5 
 
 23. Sandstone, Upper Mahoning 
 
 24. Shale 
 
 25. Coal, blossom, Mahoning 
 
 26. Concealed 50 
 
 27. Sandstone, Lower Mahoning 25 
 
 28. Shale 5 
 
 29. Coal, Upper Freeport. 
 
 Total . 
 
 Ft. in. 
 
 } 139 6 
 
 153 
 
 j> 175 
 
 80 
 
 602 
 
 Fig. 36. — Section at 
 Ligonier, Pa. 
 
 This and the preceding section, as well as the one 
 which follows, illustrate in a remarkable manner the 
 rapid variation in the individual elements of the Barrens, while the 
 total thickness remains almost exactly the same. 
 
76 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65. 
 
 Section near Berlin , Pennsylvania .— Still farther east, in the Berliu 
 basin of Somerset County, Pennsylvania, and on the very summit of 
 the Alleghany Mountains, we find this series with the following struc- 
 ture (Fig. 37) as determined by r Messrs. Platt, with some additions and 
 modifications by the writer : 
 
 l^ S "6" 
 
 •6 2V 
 ' i 
 15 ’ 
 
 446,' 
 
 Fig. 37.— Section 
 near Berlin, Pa. 
 
 Vicinity of Berlin, Somerset County , Pennsylvania. 
 
 [See map, K p.] 
 
 Ft. in. Ft. in. 
 
 ' 2 ") 
 ' 4 "\ 
 ' 6'0 
 
 1 ' 8 ") 
 0 ' 8 " > 
 V 4" > 
 
 1. Pittsburgh coal 
 
 2. Interval, shales, sandstones, etc 
 
 3. Coal 
 
 4. Limestone, gray and buff 10 
 
 5. Concealed 50 
 
 6. Sandstone, massive 25 
 
 7. Shales, dark 15 
 
 f Cannel slate 1' 1 
 
 8. Coal, Platt (crinoidal) . . j§^ slaty j- 
 
 9. Sandy shales and black slates 50 
 
 t Coal 3' 2" 
 
 10. Coal, Price (’Bakersto'wn) < Slate O' 
 
 f Coal O' 
 
 11. Slates, dark 4 
 
 f Limestone.. 1' 8"; 
 
 12. Limestone, dark gray . . < Slate 
 
 ( Limestone . 
 
 13. Shale 0 
 
 14. Coal 1 
 
 15. Shales, and concealed 45 
 
 16. Coal, Coleman 1 
 
 17. Slate, dark 0 
 
 18. Limestone, Coleman (Upper Cambridge) 
 
 19. Shales 10 
 
 20. Sandstone, and concealed 15 
 
 21. Shales, sandy 15 
 
 ( Coal V 3"1 
 
 22. Coal, Philson < Slate, black 0' 9" > 2 
 
 (Coal O' 6") 
 
 23. Fireclay 2 
 
 24. Limestone, Philaoo 5 ‘ ' V 2"'. 
 
 (Lower Cambridge)} Stalest *, s 
 
 25. Concealed, and shales 25 
 
 26. Coal, Masontown 2 
 
 27. Concealed 5 
 
 28. Sandstone, Mahoning, and concealed 100 
 
 29. Coal, Upper Freeport. 
 
 Total 
 
 200 
 
 1 
 
 ] 
 
 s 100 
 
 ;• no 4 
 
 44 6 
 
 132 
 
 599 
 
 Section at Broad Top , Pennsylvania . — As showing the remarkable 
 persistence of this series in its general thickness over the Pennsylvania 
 
WHITE. J 
 
 THE BARREN MEASURES. 
 
 77 
 
 field, we give another measurement (Fig. 38) from far east of the 
 
 Alleghany Mountains, in the center of the Broad Top 
 
 Basin, Bedford County, Report T 2 , Stevenson, page 60 : 
 
 n 
 
 Broad Top, Bedford County, Pennsylvania. 
 
 
 [See map, J t.] Ft. 
 
 1. Pittsburgh coal 
 
 2. Poorly exposed (shales and sandstones) 425 
 
 3. Sandstone, Upper Mahoning 50 
 
 4. Coal, Mahoning 5 
 
 5. Clay 3 
 
 6. Sandstone, Lower Mahoning 40 
 
 7. Coal, Upper Freeport. 
 
 Total. 
 
 523 
 
 Fig. 38. — Section 
 at Broad Top, 
 Pa. 
 
 Section opposite Steubenville , Ohio. — The next line of 
 sections in this series across the Appa- 
 lachian field will begin at Steubenville, on 
 the Ohio River, and keeping south of the 
 former line, end at Davis, Tucker County, 
 
 West Yirginia. The following succession 
 (Fig. 39) was obtained opposite Steuben- 
 ville by combining the surface observa- 
 tions with the records of drill holes and 
 shafts : 
 
 Opposite Steubenville, Ohio. 
 
 [See map, Ij.] 
 
 1. Pittsburgh coal 
 
 2. Shales, sandstone, and concealed 100 
 
 3. Shales 
 
 4. Sandstone, massive, Morgantown 
 
 5. Limestone, fossiliferous, crinoidal 
 
 6. Red shales 
 
 7. Concealed, with shales and flaggy sand- 
 
 stone < 
 
 8. Coal 
 
 9. Shale 
 
 10. Limestone, fossiliferous, Lower Cam- 
 
 bridge 
 
 11. Shales, drab 
 
 12. Shales, with coal, Masontown 
 
 13. Shales, gray 
 
 14. Sandstone, Mahoning, and concealed 
 
 under river 130 J 
 
 15. Coal, Upper Freeport. 
 
 Total 
 
 Ft. 
 
 Ft. 
 
 100 ' 
 
 ) 
 
 15 
 
 > 200 
 
 85 J 
 
 ) 
 
 10 
 
 40 ] 
 
 I 
 
 100 
 
 !> 142 
 
 1 I 
 
 
 1 J 
 
 1 
 
 8 1 
 
 2 
 
 
 5 
 
 J- 145 
 
 130 J 
 
 499 
 
 This shows a westward thinning of about 100 feet 
 for the series between Pittsburgh and Steubenville. 
 
 Section under Washington , Pennsylvania. — Near Wash- 
 ington, Pennsylvania, many wells drilled for gas and 
 oil have revealed the structure of the Barren Measures, 
 although they lie many hundred feet below the surface. 
 
 One of these borings was supervised by Prof. Lin- 
 ton, of Washington and Jefferson College, and from 
 the record thus obtained of the Thayer oil well, as 
 
 85' 
 
 200 ' 
 
 mm 
 
 v.v! 
 
 ~-Vv 
 
 !. 
 
 m 
 
 1 42' 
 
 l30’M45 r 
 
 Fig. 39. — Section 
 opposite Steuben- 
 ville, Ohio. 
 
78 
 
 THE NORTHERN BITUMINOUS COAL FIELD, 
 
 1 1 BULL. 65. 
 
 published in Pennsylvania Geological Beport, 1886, page 764, we get 
 the following for the Barrens there (Fig. 40) : 
 
 Washington, Pennsylvania . 
 
 1 . 
 
 2 . 
 
 3. 
 
 4. 
 
 5. 
 
 6 . 
 
 7. 
 
 ■ 220 * 8 . 
 9. 
 10 . 
 11 . 
 12 . 
 
 13. 
 
 14. 
 
 15. 
 
 16. 
 
 60 ' 
 
 20' 
 
 183 
 
 32f 
 
 2sr 
 
 [See map, J k.] 
 
 Ft. 
 
 Coal, Pittsburgh 
 
 Sandstone 
 
 Shale, black and red 
 
 Shale, red 
 
 Limestone 
 
 Sandstone, Morgantown 
 
 Shale, black 25] 
 
 Shale, red and variegated 
 
 Sandstone, hard 
 
 Shale, black 
 
 Sandstone 
 
 Shale, red. variegated 
 
 Sandstone, Upper Mahoning 
 
 Shale, olive green 
 
 Sandstone, Lower ( gray, fineflaggy ..15' 
 
 Mahoning. < white 17' 
 
 Shale, dark, to place for Upper I- reeport 
 coal 
 
 65] 
 70 | 
 30 > 
 5| 
 50 j 
 
 20 l 
 37 f 
 17 | 
 34 J 
 
 Ft. 
 
 220 
 
 193 
 
 28 
 
 Near Cannonshurg, Washington County, Penn 
 sylvania. 
 
 [See map, Jl.J Ft. 
 
 1. Coal, Pittsburgh 
 
 2. Limestone, blue, hard 
 
 3. Slate, white, soft 
 
 4. Shale, red 
 
 5. Slate, black 
 
 6. Shale, red 
 
 7. Sandstone, gray, hard 
 
 8. Slate, black 
 
 9. Sandstone, gray, hard, Morgantown 
 
 20 ] 
 45 I 
 36 | 
 
 47 f 
 
 IS I 
 
 38 J 
 
 Ft. 
 
 225 
 
 Fig. 40.— Section at 
 Washington, Pa. 
 
 10. Shale, red 25 ] 
 
 11. Slate, black 
 
 12. Sandstone, gray, hard 
 
 13. Slate, white, soft 
 
 14. Sandstone, gray, hard — 
 
 15. Slate, black 
 
 16. Sandstone, gray, hard 
 
 17. Slate, black 
 
 18. Sandstone, gray, hard 
 
 19. Slate, black 
 
 5 
 
 20 
 10 
 20 
 15 
 10 
 25 
 5 
 10 
 
 20. Sandstone, gray, hard 20 
 
 21. Shells and slate, gray, hard. 
 
 22. Slate, black, soft 
 
 23. Slate, with coal, Mahoning 
 
 24. Shells, gray, hard 
 
 25. Slate, black, soft 
 
 26. Sandstone, white, hard, Lower Mahoning. 
 
 27. Coal. Upper Freeport. 
 
 25 J 
 
 Total . 
 
 190 
 
 557 
 
 Total 548 
 
 Nos. 8 and 12 are the beds which 
 “cave” and give the oil drillers so much 
 trouble. 
 
 Section near Gannonsburg , Pennsylva- 
 nia . — In the vicinity of Cannonsburg, a 
 few miles northeast from Washington, 
 the record of a well drilled for gas on the 
 Boyce farm, furnished me by Mr. Wm. 
 S. Stevenson, assistant superintendent of 
 the Philadelphia Natural Gas Company, 
 gives the following (Fig. 41) as the struc- 
 ture of the Barrens there : 
 
 40 * 
 
 Fig. 41.— Section 
 near C anno n s- 
 burg, Pa. 
 
WHITE.’ 
 
 THE BARREN MEASURES. 
 
 79 
 
 Section at Morgantown , West Virginia . — From Washington across to 
 Morgantown, West Virginia, the Barren Measures, as revealed by bor- 
 ings, hold about the same thickness as in Washing- 
 ton County. In the vicinity of Morgantown the 
 entire column of the Barrens is exposed, and there 
 the following structure is exhibited (Fig. 42) : 
 
 20 
 
 227tf' 
 
 S5'6* 
 
 00 
 
 4o' 
 
 LS 7'C 
 
 Morgantoivn, Monongalia County , West Virginia . 
 
 [See map, Mm.] 
 
 1. Pittsburgh coal 
 
 2. Fire clay 
 
 3. Sandy shales and sandstone 
 
 4. Coal, Little Pittsburgh 
 
 5. Sandy shales 
 
 6. Limestone 
 
 7. Yellowish shales with iron ore 
 
 8. Sandy shales, and concealed 
 
 9. Sandstone, rather massive 
 
 10. Sandy shales, and concealed 
 
 11. Massive sandstone 
 
 12. Bluish green sandy beds 
 
 13. Black slate, fossiliferous 
 
 14. Limestone, Clarksburg 
 
 15. Shales and sandy beds 
 
 16. Sandstone, Morgantown 
 
 17. Elk Lick coal 
 
 18. Shales, and concealed 
 
 19. Limestone, crinoidal 
 
 20. Variegated shales 
 
 21. Limestone, Upper Cambridge 
 
 22. Shales.. 
 
 23. Sandstone, Upper Mahoning 
 
 24. Shales and slialy sandstone. . . r 
 
 25. Massive sandstone, Lower Mahoning. 
 
 26. Shales 
 
 27. Coal, Upper Freeport. 
 
 Total 
 
 227 
 
 Ft. in. Ft. in. 
 
 2 1 
 32 
 1 
 
 17 
 1 
 
 10 
 17 
 25 
 15 
 20 
 20 
 1 
 1 
 45 
 20 
 
 3 
 55 
 
 1 
 
 85 
 
 1 
 
 14 ! 
 
 3 6 | 
 
 30 
 100 
 40 
 
 187 
 
 561 
 
 The black fossiliferous slate, No. 13, represents 
 fig. 42.— section at Mor- the horizon of the Little Clarksburg coal, and is 
 here filled with fish teeth and scales. The Ujpper 
 Freeport coal is about 100 feet under the river at the Morgantown 
 wharf, but southward it rises very rapidly and comes up to the bed of 
 the river at the mouth of Coburn’s Creek, 2 miles above. It is there 
 about 4 feet thick and very pure. 
 
80 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65. 
 
 Section near Little Falls , West Virginia . — In the vicinity of Little 
 Falls, Monongalia County, 9 miles above Morgantown, the basal mem- 
 bers of the Barrens can be obtained more in detail 
 than in the Morgantown section, and the following 
 (Fig. 43) shows the structure there : 
 
 Little Falls, Monongalia County , West Virginia. 
 
 , * [See map, 
 
 m.] 
 
 47 ' 
 
 
 a*.' 
 
 
 =.== 24 , 6 " 
 
 s- iz' >9a'a' 
 
 Z6'6" 
 
 Fig. *43. — Section at Lit- 
 tle Falls, W. Va. 
 
 1. Pittsburgh coal 
 
 2. Shales, sandstones, and concealed . . . 
 
 3. Sandstone, in knob 
 
 4. Shales 
 
 5. Massive, coarse yellow sandstone — 
 
 6. Coaly shale, Little Clarksburg 
 
 7. Limestone, fossiliferous, Clarksburg 
 
 8. Concealed, shales and sandstone 
 
 9. Limestone, nodular 
 
 10. Gray and yellow shales 
 
 Ft. in. Ft. in. 
 
 ) 
 
 100 
 
 5 
 
 15 
 
 21 
 
 0 
 
 1 
 
 47 
 
 3 
 
 .macK siate 
 
 I 
 
 f ( Coal 
 
 ... 12") ) 
 
 
 j Coal . < Slate 
 
 ... 1"> V 5" 
 
 Coal, Elk Lick . { 
 
 t Coal 
 
 . . . 4" S S 
 
 Concealed with red shale. 15' 
 
 • i 
 
 ' Coal, good 
 
 O' 6" j 
 
 13. Shales 
 
 14. Limestone, gray and buff in several layers, Elk Lick. 
 
 15. Flaggy sandstones and shales 
 
 16. Sandstone, massive, pebbly at base for 4 feet 
 
 17. Concealed, probably shales , 
 
 18. Fossiliferous shale, crinoidal 
 
 19. Concealed, red shales and impure limestones 
 
 20. Limestone, light gray, TJpper Cambridge 
 
 21. Shales and flaggy sandstones 
 
 22. Sandstone, rather massive 
 
 23. Concealed, and shales 
 
 24. Sandstone, Upper Mahoning, massive 
 
 25. Coal, Mahoning 
 
 26. Shales and concealed 
 
 27. Shale, greenish, sandy , 
 
 28. Sandy shale and flaggy sandstone 
 
 29. Shale, greenish yellow 
 
 30. Concealed, probably shale 
 
 31. Lower Mahoning sandstone 
 
 32. Coal, Upper Freeport. 
 
 Total 
 
 205 9 
 
 6 
 
 22 10 
 
 15 
 
 31 
 
 24 6 
 
 10 10 
 
 16 11 
 
 83 4 
 
 10 
 
 65 6 
 
 1 
 
 16 3 f 106 1 
 
 53 6 j 
 
 27 1 
 
 11 
 
 5 2 I 
 
 12 
 17 
 
 26 o j 
 
 98 8 
 
 587 3 
 
 This section illustrates well the variability of the Barren Measures, 
 when compared with the previous one, taken only a few miles distant. 
 
WHITE.] 
 
 THE BARKEN MEASURES. 
 
 81 
 
 Section at Newburg , West Virginia . — The syncline between the Chest- 
 nut Ridge and Laurel Hill anticlines crosses the Baltimore and Ohio 
 Railroad at Newburg, Preston County, West Virginia, 
 about 15 miles east from Little Falls, and there the 
 Barren Measures admit of vertical measurement by 
 combining surface exposures with the record of the 
 Orrel Coal Company’s shaft. The result is as follows 
 (Fig. 44) : 
 
 2J0 
 
 
 Newburg, Preston County, West Virginia . 
 
 [See map, N m.] 
 
 iS' 
 
 r 
 
 20 ' 
 
 5‘ 
 
 4o 
 
 to' 
 
 1$’ 
 
 20 ' 
 10 f 
 10' 
 
 I o' 
 
 J5’ 
 
 95 
 
 aor 
 
 61) 
 u a 
 ga 
 g ° 
 ©.a 
 
 ^3 
 
 1. 
 2. 
 
 3. 
 
 4. 
 
 5. 
 
 6 . 
 
 7. 
 
 8 . 
 
 9. 
 
 10 . 
 11 . 
 12 . 
 
 13. 
 
 14. 
 
 15. 
 
 16. 
 
 17. 
 
 18. 
 19. 
 
 3 ] 20 . 
 
 l| 21 - 
 
 P 122. 
 
 23. 
 
 24. 
 
 25. 
 
 26. 
 27. 
 
 fci ( 
 "a 
 
 Pittsburgh coal 
 
 Fire clay 
 
 Concealed 
 
 Shales, sandy 
 
 Concealed 
 
 Sandstone, pebbly, Morgantown 
 
 Concealed 
 
 Sandstone, flaggy 
 
 Shales, sandy 
 
 Shales, dark, fossiliferous (crinoidal) 
 
 Concealed 
 
 Red, marly shale 
 
 Concealed 
 
 Sandstone, yellow 
 
 Concealed - 
 
 Fire clay and shales 
 
 Sandstone, massive 
 
 Sandy shale 
 
 Sandstone, massive 
 
 Concealed 
 
 Sandstone 
 
 Shales 
 
 Coal, Mahoning 
 
 Sandstone — 
 
 Shale 
 
 28. 
 
 Sandstone 
 
 Shale 
 
 Sandstone 
 
 Coal, Upper Freeport. 
 
 Ft. 
 
 5 ) 
 
 14 I 
 
 30 > 
 230 j 
 30 J 
 
 15 1 
 
 1S [ 
 
 10 J 
 
 20 
 
 5 
 
 40 
 
 10 \ 
 15 
 
 5 ) 
 20 ) 
 10 
 10 
 10 f 
 
 35 I 
 25 J 
 
 34 > 
 1 | 
 3 J 
 
 Total . 
 
 80 
 
 Ft. 
 
 •309 
 
 35 
 
 15 
 
 95 
 
 no 
 
 80 
 
 645 
 
 This is in the same geological trough as the section 
 at Ligonier (Fig. 36), and, as will be observed, agrees 
 Fl Newbm-g 6 w°va at ^ * n having an unusually large interval between 
 
 the Pittsburgh coal and the base of the Morgantown 
 sandstone. It is possible that the Upper Mahoning sandstone should 
 not include Nos. 17-20 at thjs locality. 
 
 Bull. 65 6 
 
82 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section near Fairfax Knob , West Virginia .— About 50 miles east 
 from Newburg we come to the North Potomac Coal Basin, the south- 
 ward extension of the Cumberland or Georges Creek 
 field of Maryland, and there, in the vicinity of Fairfax 
 Knob, Tucker County, West Virginia, the Barrens ex- 
 & hibit the following structure (Fig. 45) : 
 
 Fairfax Knob, Tucker County, West Virginia. 
 
 [See map, O o.] 
 
 
 Ft. 
 
 1. Pittsburgh, coal 
 
 2. Shales and concealed 
 
 Ft. in s 
 
 85 
 
 ( Coal 2' 9" ■ 
 3 Coal, Little Pittsburgh . . < Slate . 0' 6" ( 
 (Coal.. O' 6" . 
 
 4. Shales 
 
 5. Coal 
 
 f Coal, slaty. 0' 10” 1 
 
 j Coal 1' 5" 1 
 
 i Slate V 0” ( * 
 
 I Coal V 0”J • 
 
 6. Fire clay and shalgs 
 
 7. Blue shales with iron ore 
 
 8. Black slate 
 
 
 C Coal.. O' 8”} 
 
 9. Coal, Little Clarksburg . . < Slate . O' 4” V 
 
 (Coal. 1' 0” ) 
 
 10. Concealed, with sandstones and shales 
 
 11 . Coal, and black slate, Masontown 
 
 12. Shales 
 
 f 13. Sandstone, massive 
 
 ! 14. Concealed ® 
 
 l 15. Sandstone, soft 1 
 
 y . 
 
 ^ ^ I 16. Clay, yellow 
 
 [ 17. Sandstone 
 
 18. Limestone, Mahoning . 
 Soft shale 
 
 u fl9' 
 
 •g 20. Hard shale 
 
 21. Soft shale 
 
 ^ s , 22. Slate, light blue. 
 23. Slate, dark 
 
 [24. Sandstone 
 
 25. Coal, Upper Freeport. 
 
 20 
 
 1 
 
 9 
 
 1 
 
 10 
 
 19 
 
 2 
 
 Total 
 
 40 
 
 200 
 
 3 
 
 50 
 
 61 
 
 20 
 
 42 
 
 538 
 
 Fig. 45. — Section at 
 Fairfax knob, W. 
 
 Va. 
 
 The last 100 feet of the section was obtained from the record of a 
 diamond drill hole put down by the West Virginia Central Railroad 
 to test the character of the Upper Freeport coal. The writer saw sam 
 pies of the Mahoning limestone, taken from the drill hole, and it was 
 
 a dark gray, rather pure limestone. 
 
 No. 5 is a second Little Pittsburgh coal which is occasionally present 
 in the Potomac basin and elsewhere. 
 
WHITE.] 
 
 THE BARKEN MEASURES. 
 
 83 
 
 Section in Guernsey County , Ohio . — Toward the northwestern side of 
 the Appalachian basin, in Ohio, the Barrens are thinner than elsewhere, 
 as may be seen from the following section (Fig. 46), 
 made by Mr. F. W. Minshall, in Guernsey County, 
 Ohio. 
 
 (Guernsey County , Ohio. 
 
 [See map, Kf.] 
 
 Ft. in. 
 
 1. Pittsburgh coal 
 
 2. Shales 10 
 
 3. Limestone 15 
 
 4. Shales 30 
 
 5. Concealed 75 
 
 6. Shales 20 
 
 7. Limestone, crinoidal 
 
 8. Coal, crinoidal 1 3 
 
 Ft. in. 
 
 > 150 
 
 | 
 
 9. Shales 15 
 
 mb'? 10. Limestone 
 
 10 
 
 11. Shales 35 
 
 12. Sandstone, pebbly . 25 
 
 13. Shales 5 
 
 14. Coal, Bakerstown 2 
 
 15. Shales 35 
 
 16. Limestone, Lower Cambridge. . 
 
 17. Shales -. 5 
 
 18. Coal, Masontown 1 
 
 19. Shales 30 
 
 20. Sandstone, Upper Mahoning. . . 35 
 
 21. Coal, Mahoning 1 
 
 22. Shales 5 
 
 23. Sandstone, Lower Mahoning. . . 30 
 
 24. Shales 5 
 
 25. Coal, Upper Freeport. 
 
 Total 
 
 > 112 11 
 
 395 2 
 
 Fig. 46. — Section in 
 Guernsey County, 
 Ohio. 
 
 Section at Burning Springs , West Virginia . — At Burn- 
 ing Springs, Wirt County, West Virginia, the Barren 
 Measures have the following structure (Fig. 47), ac- 
 cording to Mr. Minshall: 
 
 Burning Springs , Wirt County , West Virginia. 
 
 [See map, P g.] 
 
 Ft. in. Ft. in. 
 
 1. Pittsburgh coal 
 
 2. Shales 10 ] 
 
 3. Limestone 10 j> 200 
 
 4. Concealed 180 j 
 
 5. Limestone, crinoidal 3 
 
 6. Coal, crinoidal 1 8 ) 
 
 7. Shales 10 
 
 8. Limestone 3 ! 
 
 9. Concealed 200 / 294 8 
 
 10. Sandstone 40 
 
 11. Shales 40 | 
 
 12. Coal, Upper Freeport. 
 
 Total 407 8 
 
 
 Fig. 47. — Section at 
 Burning Springs, W. 
 Va. 
 
84 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section near Huntington , West Virginia . — Near the southwestern 
 limit of the district, in the vicinity of Huntington, West Virginia, the 
 Barren Measures have the following structure (Fig. 
 48) according to the determinations of Mr. A. G. 
 Selby, who made careful measurements of the rocks 
 exposed there, and combined them with the record 
 of a boring for gas : 
 
 ■Rl 
 
 197' 
 
 185* 
 
 Vicinity of Huntington , West Virginia , along Ohio River. 
 
 [See map, S b.] 
 
 1. Pittsburgh coal 
 
 2. Red shale, contaiuing limestone nodules 
 
 3. Sandstone, skaly 
 
 4. Red shales and shalv sandstone 
 
 5. Coal, Little Clarksburg 
 
 6. Sandstone, massive, Morgantown 
 
 7. Elk Lick coal 
 
 8. Fireclay 
 
 9. Shales, deep red 
 
 10. Limestone, crihoidal 
 
 11. Coal, crinoidal 
 
 12. Red shales 
 
 13. Limestone 
 
 14. Shales and sandstones 
 
 15. Limestone, Lower Cambridge 
 
 16. Shales 
 
 17. Coal, Masontown 
 
 18. Shales 
 
 19. Sandstone, Mahoning 
 
 20. Upper Freeport coal. 
 
 Total 
 
 Ft. 
 
 28 
 
 16 
 
 101 
 
 2 
 
 50 
 
 3 
 
 103 
 
 2 
 
 4 
 4 
 
 175 
 
 10 
 
 1 
 
 30 
 
 125 
 
 Ft. 
 
 197 
 
 2 
 
 106 
 
 2 
 
 185 
 
 2 
 
 166 
 
 Fig. 48.— Section near 
 Huntington, W.Va. 
 
 This is nearly twice the thickness that the Ohio 
 geologists report for the Barrens along the north- 
 western margin of their outcrop, but all of the meas- 
 ures thicken very rapidly toward the southeast from 
 this portion of Ohio. It is possible, however, that 
 Mr. Selby may have gotten some of the elements of 
 the section too thick, since there is no single point 
 between Huntington and the Big Sandy where a ver- 
 tical measurement of all the members can be made. 
 The true thickness can not be much under 600 feet at 
 least. 
 
WHITE.] 
 
 THE BARREN MEASURES. 
 
 85 
 
 Section near Charleston , West Virginia. — In the vicinity of Charleston, 
 West Virginia, and just north from it, the Barren Measures attain a 
 greater thickness than anywhere else in the Appala- 
 chian Basin, so far as known. The following structure 
 (Fig. 49) may be observed along the Great Kanawha 
 Kiver there, and its tributary, Two- mile Creek : 
 
 Near Charleston, West Virginia. 
 
 fSee map, S f.] 
 
 
 Ft. 
 
 Pittsburgh coal - 
 
 Concealed red shales and sandstone.-. 140 
 
 Sandstone, massive 30 
 
 Red shales, sandstone and concealed 150 
 
 Coal, Elk Lick 
 
 Shales 
 
 Sandstone 
 
 Shales, marly, with limestone nodules 
 
 Limestone, impure (crinoidal horizon) 
 
 Dark red shales with iron nodules 
 
 Shales 
 
 Coal, impure, Bakerstown 
 
 Eire clay and shales 
 
 Sandstone, massive, pebbly 
 
 Shales and sandstone 
 
 Shales, with streaks of coal, Masontown 
 
 Sandstone, very hard ,-••?- ■ 
 
 Coal, Mahoning . . . .4. F. . . .* 
 
 Massive sandstone 
 
 Shales 
 
 Coal, Upper Canneltonr. . .( .4r. F >. . 
 
 Sandstone, massive. 
 
 Sandy shales , 
 
 Coal, Middle Cannelton >. K . .'A Jl 
 
 Black flint 1 
 
 Shales .. 
 
 Coal, Upper Freeport. 
 
 10 
 
 30 
 
 30 
 
 30 
 
 25 
 
 5 
 
 5 
 
 30 
 
 100 
 
 20 
 
 25 
 
 4 
 
 75 
 
 10 
 
 2 
 
 50 
 
 15 
 
 1 
 
 5 
 2 
 
 Ft. 
 
 320 
 
 1 
 
 70 
 
 5 
 
 ► 215 
 
 1 
 
 Total . 
 
 800 
 
 
 7 s’ 
 
 iliil 
 
 
 
 
 
 vS 
 
 
 so* 
 
 m 
 
 15' 
 
 
 V j 
 
 Fig. 49.— Section near Charleston, W. Va. 
 
 As may be seen from these sections 
 just given, many of the beds which have 
 received distinct names are not persist- 
 ent. They occur at some localities but 
 are wanting in others, and hence are so 
 variable that they are never all found in 
 one section. 
 
 We shall now take up the more im- 
 portant members of the series and de- 
 scribe them in more detail as exhibited at 
 their type localities and elsewhere. 
 
86 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 CHARACTERISTIC HORIZONS. 
 
 THE PITTSBURGH COAL ORES. 
 
 In Fayette County, Pennsylvania, a group of iron ores come immedi- 
 ately below the Pittsburgh coal, and have been mined for the manufac- 
 ture of iron for nearly 75 years. They have been very carefully studied 
 by Stevenson, who describes them in his report (KK) of the Pennsylva- 
 nia Geological Survey. He gives the following as the general section 
 of the ores : 
 
 Pittsburgh coal 
 
 Clay 
 
 Blue Lump ore 
 
 Clay ... 
 
 Condemned flag ore 
 
 Clay 
 
 Big Bottom ore 
 
 Clay 
 
 Red flag ore 
 
 Clay 
 
 Yellow flag ore 
 
 2 to 8 feet. 
 
 1 to 0 foot. 
 
 4 inches to 1 foot 6 inches. 
 
 1 to 0 foot. 
 
 . 4 inches to 2 feet 6 inches. 
 ...1 foot to 1 foot 8 inches. 
 
 10 inches to 5 feet. 
 
 2 inches to 6 feet. 
 
 1 to 3 feet. 
 
 4 inches. 
 
 This succession does not, of course, represent the structure of the ore 
 layers at all localities, as the thickness and quality are constantly vary- 
 ing. 
 
 The “ Blue Lump ” and the “ Big Bottom ” beds are of the most im- 
 portance, and it is from the former one especially that Mr. F. H. Oli- 
 phant manufactured iron so long and successfully at Fairchance. 
 These ores are confined principally to the Blairsville basin, in Fayette 
 County, though they extend into the edge of Monongalia County to the 
 south, and have been recognized on the edge of Greene County to the 
 west. 
 
 When these ores are not present their places are often occupied by 
 ferruginous limestones or shales, though occasionally a sandstone 
 stratum comes in close under the coal and cuts out everything else. 
 This interval, immediately below the Pittsburgh, for 30 to 40 feet is 
 more variable than any other portion of the Barrens, and hence it is 
 useless to attempt to classify its rocks. 
 
 THE LITTLE PITTSBURGH COAL. 
 
 At a varying interval of 25 to 60 feet from the top of the Barrens 
 there often occurs a thin and usually impure coal bed, which has been 
 termed the Little Pittsburgh coal, from the fact that it is so close to 
 the great bed above. The thickness selc.om exceeds two feet, and it is 
 often only half that. The best development of this coal which the 
 writer has ever seen occurs in Fairfax Knob, Tucker County, West : 
 Virginia, at the locality of Section 45, where the bed is nearly 4 feet 
 thick and is locally known as the “ coking vein,” from the fact that it 
 has the typical structure of a good coking coal. 
 
 • 
 
 M 
 
WHITE.] 
 
 THE BARREN MEASURES. 
 
 87 
 
 Occasionally there appear to be two of these beds, one at 20 to 30 
 feet below the Pittsburgh and the other at 50 to 75 feet below, but 
 they may probably both be splits from the same bed. 
 
 The Little Pittsburgh coal is quite persistent at the northern end of 
 the Appalachian coal basin, but it disappears south westward across 
 West Virginia and is seldom seen beyond Harrison County. It also 
 fades away southward in Ohio, since it does not appear in any of the 
 Ohio sections, unless it should be the “ Jeffers” coal of Prof. Andrews, 
 in Gallia County. That, however, may possibly represent the Pitts- 
 burgh bed. In the vicinity of Wellersburg, Somerset County, Penn- 
 sylvania, there appear to be two of these Little Pittsburgh beds, and 
 the upper contains 3 to 4 feet of good coal, while the lower is only 18 
 inches thick. 
 
 THE PITTSBURGH LIMESTONES. 
 
 There are very frequently two limestones in the shale interval of 50 
 to 75 feet below the Pittsburgh coal, one of which comes above. the 
 Little Pittsburgh coal and the other a few feet below. They are both 
 known under the general name of Pittsburgh limestone ; but it would 
 be better to call the first one Upper Pittsburgh and the other one 
 Lower Pittsburgh. The first is seldom more than 3 to 5 feet thick, but 
 the latter is occasionally much thicker, as it is the more persistent of 
 the two, being purer and frequently quarried and burned into lime for 
 agricultural and other purposes. 
 
 THE CONNELLSVILLE SANDSTONE. 
 
 At a short interval under the Lower Pittsburgh limestone there is 
 often found a massive sandstone which is frequently conglomeritic. 
 This rock rises from the bed of the Youghiogheny River at Counells- 
 ville, and was named from that locality by Dr. Stevenson. Being one 
 of the cliff rocks in the Barren Measures, it has played an important 
 part in shaping their topography. It is especially hard and massive 
 in the Cumberland or Georges Creek basin, and the rounded hills 
 which hold the “Big” (Pittsburgh) “vein” rest on a platform of this 
 rock, which, owing to its erosion-resisting power, makes a bold terrace 
 far uj) the mountain sides after all the soft beds above have disappeared. 
 It is this great bed of pebbly sandstone that caps the summits in the 
 center of the trough south from Elk Garden, after the Pittsburgh coal 
 has disappeared, forming almost level plateaus over thousands of acres 
 where the great Pittsburgh bed is missed by an interval of only 50 to 
 60 feet. 
 
 The same pebbly sandstone marks the summits of the hills at Beling- 
 ton, Barbour County, West Virginia, and forms huge cliffs at many 
 points along the Monongahela River between Fairmont and Morgan- 
 town. 
 
 At Connellsville the top of this stratum lies about 60 feet under the 
 Pittsburgh coal ; but this interval is sometimes as small as 40 feet, and 
 
88 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [mull. 65 . 
 
 again increases to 80 or 90. When not pebbly it frequently furnishes 
 excellent building stone. The thickness varies from 25 to 50 feet, but 
 it is often absent as a massive rock, and then its place is filled with 
 sandy shales or flaggy sandstone. 
 
 THE LITTLE CLARKSBURG COAL. 
 
 By this name has been designated a bed of slaty coal which occa- 
 sionally makes its appearance close under the Connellsville sandstone, 
 and 100 to 125 feet below the Pittsburgh coal. 
 
 At Clarksburg, West Virginia, the coal in question crops out along 
 the bed of Elk Creek for a considerable distance, and is 1J to 2 feet 
 thick, but poor and slaty. It is called Little Clarksburg to distinguish 
 it from the Pittsburgh coal, which is extensively mined in the vicinity 
 of that town, and is locally known as the Clarksburg bed. 
 
 Very frequently this coal is represented by a bed of black slate, 
 which is filled with fish remains, teeth, scales, etc. The deposit in 
 question is rarely more than 1J to 2 feet thick, and is often absent 
 altogether, so that it is of very little economic importance, though in 
 the Wellersburg region of Somerset County, Pennsylvania, it attains 
 a thickness of nearly 6 feet, and contains some good coal, being known 
 as the “G-foot” bed. 
 
 THE CLARKSBURG LIMESTONE. 
 
 Directly under the last described coal there often occurs a limestone 
 which is finely exposed in the vicinity of Clarksburg, along the bed of 
 Elk and the West Fork Biver. The upper portion is there rather 
 slaty, and filled with fossil ostracoids and fish remains. The next layers 
 under this are very compact, and come out in peculiar rhomboidal 
 blocks. This entire limestone series is 20 to 30 feet thick, and some of 
 the layers are quite ferruginous, so much so that they were mined for 
 ore many years ago at an old charcoal furnace on Elk. Some iron ore 
 was also obtained near Clarksburg from the roof shales just above the 
 Little Clarksburg coal, and used in this furnace. The Clarksburg 
 limestone is rather widely distributed in Pennsylvania and northern 
 West Virginia, and is frequently mined, since many of its layers fur- 
 nish good lime for fertilizing and building purposes. 
 
 THE MORGANTOWN SANDSTONE. 
 
 At 25 to 40 feet under the Clarksburg limestone, and separated from 
 it by soft shales, we find one of the great sandstone horizons of the 
 Barren Measures. This rock was named by Dr. Stevenson from its 
 fine exposure at Morgantown, West Virginia, where it has been exten- 
 sively quarried and used in building the State University and other 
 structures. At this typical locality the top of the stratum lies about 
 200 feet below the Pittsburgh coal, and the thickness of the sandstone 
 is 25 feet. It is of a yellowish gray cast, of medium grain and hard- 
 ness, and splits readily into blocks of any desirable size. Scattered 
 
WHITE.] 
 
 THE BARREN MEASURES. 
 
 89 
 
 through the rock are stains of peroxide of iron and also a considerable 
 quantity of feldspar graius, which are generally decomposed, thus 
 giving the surface of the stone a mealy look. In some of’ the crevices 
 and cavities of the sandstone pure kaolin has accumulated from this 
 source. The base of the sandstone is often conglomeritic and some- 
 times brecciated. 
 
 This is a quarry sandstone nearly everywhere that its outcrop ex- 
 tends. All along the Monongahela River it has been quarried and 
 used in building the locks of the Slack Water Company. The stone 
 dam, No. 9, was built of rock from this stratum. It is one of the most 
 persistent members of the Barren Measures, and often makes high 
 cliffs. It caps the hills in the vicinity of Grafton, West Virginia, 
 where it is also quarried, and it makes a line of conspicuous bluffs from 
 there to beyond Newburg, along Three Fork, and far up into Barbour 
 County along the Valley River. Along the North Potomac River, in 
 Mineral, Grant, and Garrett Counties, the same rock is found, and on 
 the Great Kanawha, Guyandotte, Big Sandy, Big and Little Muskin- 
 gum, and other tributaries of the Ohio, this bed is generally conspicu- 
 ous. At Huntington, West Virginia, on the banks of the Ohio, it is 50 
 to 60 feet thick, while on Crooked Run, Monongalia County, near the 
 Pennsylvania line, the stratum is 100 feet thick. It is the first oil rock 
 on Dunkard Creek, and some of the wells produced largely from it. In 
 the deep borings of Washington County, Pennsylvania, where it under- 
 lies the surface 500 to 1,000 feet, this stratum is 35 to 50 feet thick, and 
 generally contains salt water. 
 
 THE ELK LICK COAL. 
 
 Immediately under the Morgantown sandstone, or separated from it 
 by only a few feet of shale, there comes a coal of very wide distribution 
 which occasionally attains workable dimensions. 
 
 This name was given the coal in question by the First Geological Sur- 
 vey of Pennsylvania, but the place of the bed in the series remained 
 uncertain till Messrs. Platt, of the Second Survey, recently deter- 
 mined the matter finally by identifying the massive sandstone above it 
 at the typical locality as the Morgantown. 
 
 This coal attains a thickness of 4 feet in Somerset County, Penn- 
 sylvania, and has there been mined to a considerable extent for local 
 use. 
 
 In Westmoreland, Fayette, and Alleghany it seldom exceeds 2 feet, 
 and is generally less, but quite persistent. 
 
 In Preston County, West Virginia, north from Cheat River, this bed 
 has been mined to a considerable extent and is known as the u top 
 vein.” In the summits near Bruceton it is 4 feet thick and a rather 
 good coal. 
 
 At Morgantown it is nearly 4 feet thick, but rather poor and slaty. 
 
 South from Monongalia County, it is occasionally seen, but is not so 
 
90 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65. 
 
 thick as at the northern end of the field. At Glenville, Gilmer County, 
 it is in the bed of the Little Kanawha Biver, and 18 to 20 inches thick. 
 
 The same coal is also recognizable on the Big Kanawha, but is there 
 quite thin. In the section (48) at Huntington, West Virginia, Mr. 
 Selby finds this coal 2 feet thick but very slaty. 
 
 It is not often reported by the Ohio geologists, and hence may fre- 
 quently be absent from the measures in that State. 
 
 THE ELK LICK LIMESTONE. 
 
 In sections 37 and 43, a limestone is seen at a short interval below 
 the Elk Lick coal, and from its occurrence at this hori zon in Somerset 
 County, Pennsylvania, it has been termed the Elk Lick limestone by 
 Mr. Franklin Platt, of the Second Geological Survey, Pennsylvania. 
 The stratum in question occurs at 200 to 240 feet under the Pittsburgh 
 coal, and is not always present. 
 
 As exhibited in Somerset County, Pennsylvania, this limestone is of 
 a light gray color, and often tinged with buff, the same being true of it 
 in Monongalia. Platt reports it as 12 feet thick in Somerset, but in 
 Monongalia it is only about half that, and is not persistent. 
 
 THE CRINOIDAL LIMESTONE (GREEN FOSSILIFEROUS LIMESTONE, AMES LIMESTONE). 
 
 The next step downward in the rocks takes us to a very important 
 horizon and one which marks a change from fresh or brackish water 
 deposits to marine conditions, for here we get abundant marine fossils 
 for the first time in descending the column of rocks. 
 
 The bed in which these fossils occur has received several names. 
 The geologists of the First Geological Survey of Pennsylvania called 
 it the Green Fossiliferous limestone, the Ohio Survey has termed it the 
 Ames limestone, while the Second Geological Survey of Pennsylvania 
 has termed it the Crinoidal limestone. This latter name is so well 
 known now in geological literature that it is probably best to let it stand, 
 though as a synonym and geographical designation the Ames lime- 
 stone may be retained. 
 
 The character of this stratum and its fossils have been admirably 
 worked out by Stevenson, who first showed its importance as a strati- 
 graphical horizon. It comes almost exactly midway in the Barren 
 series, and hence it is a constant datum from which the geologist can 
 measure either upward or downward to identify the rocks. 
 
 When once thoroughly known it can not be confused with any other 
 rock in these measures, since it is the highest bed that coutains abun- 
 dant Brachiopods and Lamellibranclis, and its lithology is distinctly dif- 
 ferent from anything else. Prof. Stevenson thus aptly describes its 
 general features : “ Dark bluish or greenish gray, tough, and breaks 
 with a granular surface much resembling that of a coarse sandstone. 
 * * *. In all cases it is fossiliferous and contains immense numbers 
 
 of crinoidal stems and spines or plates.” 
 
WHITE.) 
 
 THE BxlRREN MEASURES. 
 
 91 
 
 Its common fossils are: Productus Nebrascensis , P. Prattenianus , P. 
 longispinus , P. semi-reticulatus , Hemipronites crassns, Spirifera earner ata, 
 S. piano eonvexa, Athyris subtilita , Lophophyllum proliferum , Zeacrinus 
 mucrospinus , together with the undetermined plates and stems of cri- 
 noids. 
 
 Throughout Pennsylvania this stratum comes about 275 to 300 feet 
 below the Pittsburgh coal, and the same distance above the Upper 
 Preeport, though occasionally this last interval is increased to 350 feet. 
 The rock is rarely more than 2 feet thick, and often not so much, but is 
 wonderfully persistent. Even when not present as limestone its hori- 
 zon is almost invariably made known by the fossiliferous shales which 
 accompany the bed. 
 
 Through Ohio thjs rock is almost continuously present from the point 
 where it enters the State near Steubenville clear around to where it 
 leaves it at the Kentucky line near Catlettsburg. 
 
 Opposite Steubenville the bed is 8 to.10 feet thick, but this is unusual, 
 since it is only 1 to 3 feet at most points in Ohio. 
 
 The interval between this rock and the Pittsburgh coal decreases 
 westward to 200 feet on the Ohio River at Wellsburg, and farther west 
 in Ohio the interval still further declines to 140 feet, but where it leaves 
 the State at the southwest it increases again and gets to be 300 feet 
 opposite Huntington, West Virginia. 
 
 Through this latter State the limestone holds its place very regularly 
 in the series from the Pennsylvania line southward into Harrison and 
 Lewis Counties, and it is also present on the Volcano uplift at Burn- 
 ing Springs and other points, still holding its characteristic fossils. It 
 disappears, however, in passing from this Little Kanawha region south- 
 ward to the Big Kanawha, for when we come to this latter stream the 
 fossiliferous limestone is gone, and its horizon replaced near Charles- 
 ton by a thin, impure limestone which holds only minute fresh water 
 forms. It is highly probable, however, that the crinoidal bed comes in 
 again a few miles north from Charleston, since on the Big Sandy it was 
 followed 20 to 25 miles above the mouth of that stream, and there it 
 still retains its crinoidal phase, though getting very impure where last 
 seen in that valley. 
 
 THE CRINOIDAL COAL. 
 
 Immediately under the last described limestone we very often find a 
 thin coal bed, which seldom exceeds 18 inches in thickness, and hence 
 is of very little economic importance. In Somerset County, Pennsylva- 
 nia, Mr. Franklin Platt identified with this coal No. 8 of the Berlin (37) 
 section, a very impure, slaty bed, occurring in several layers in the vi- 
 cinity of Berlin, where it is altogether 7 feet thick, and locally known 
 as the Platt coal. If this identification be correct, this is the greatest 
 development the coal ever attains. 
 
 There is only one other locality besides the Berlin region where 
 this coal has been mined to any considerable extent, and that is at 
 
92 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Burning Springs, Wirt County, West Virginia. Here it was mined 
 aud used for fuel iu drilling the numerous oil wells once put down there, 
 and it is still taken out on a small scale for domestic purposes, though 
 only 20 inches thick. Some very finely preserved fossil Brachiopods 
 and Lamellibrauchs have been obtained from the roof shales of the 
 coal at Burning Springs, since it there comes only 2 to 5 feet below the 
 Crinoidal liihestone. 
 
 The u Weller” coal, near Wellersburg, Pennsylvania, is probably 
 identical with this bed. 
 
 RED SHALE BEDS. 
 
 Throughout most of the Pennsylvania and West Virginia region, the 
 Crinoidal limestone is underlaid by very soft, red, and variegated shales, 
 and marly clays. They make a broad red band in the soil wherever 
 they extend, and are a great nuisance along roads and railroads, since 
 when wet they decompose into a greasy mud, which produces many 
 landslides and slips. 
 
 It is this stratum which causes so much trouble to the oil and gas 
 drillers of southwestern Pennsylvania aud the adjoining regions of 
 West Virginia, since it is so easily reduced to mud, which runs into the 
 hole and fills it up, so that casing must be put through the stratum as 
 soon as the drill has penetrated it. From this tendency to slide out 
 into the drill hole, it is termed by the oil drillers the u caving” rock. 
 
 Over a large portion of Ohio and in many regions of West Virginia 
 a hard, bluish gray limestone, not at all or but sparingly fossiliferous, 
 occurs near the center of this shale interval. The bed is 3 to 10 feet 
 thick, and in Ohio is generally called the Ewing limestone. It is shown 
 in the West Virginia sections at Burning Springs (47) and at Hunting- 
 ton (48), and it is recognizable at many other points in the State. 
 
 The rest of the Barren Measures from this red shale down to the Ma- 
 honing sandstone is extremely variable. ’Sometimes it is nearly all 
 shales, much of which is red, and u caves ” in drilling through it, just 
 like that under the Crinoidal limestone, and again as in the Berlin sec- 
 tion (37) it contains 3 or 4 coal beds, and as many limestones. Some of 
 these, however, are rather persistent and will be referred to in detail. 
 
 THE BAKERSTOWN COAL. 
 
 At some localities in western Pennsylvania a bed of coal is found 75 
 to 90 feet uuder the Crinoidal limestone. This bed is mined in the vi- 
 cinity of Bakerstown, Alleghany County, and it has been designated 
 from that village. As there exhibited, it is not quite 3 feet thick and 
 rather slaty. In the Berlin region a coal called the Price bed seems to 
 come at this horizon. It is about 4 feet thick and furnishes some val- 
 uable fuel in Somerset County. 
 
 Iu Section 37 will be found some thin coal beds under the Price coal, 
 which are rarely represented in any other section of the Barrens. 
 
WHITE.] 
 
 THE BARREN MEASURES. 
 
 93 
 
 Among these are the Coleman, Philson, and the one a few feet under 
 the Price bed; but they are all local, though occasionally we find traces 
 of some of them in other regions than Somerset County. This whole 
 interval for 100 feet below the Crinoidal limestone is so extremely vari- 
 able that the classification for one region is of very little use in another. 
 An instance of this is seen at Saltsburg, Pennsylvania, where a great 
 sandstone 100 feet thick comes into the series a few feet under the 
 Crinoidal limestone horizon. This was termed the Saltsburg sandstone 
 by Stevenson, but it is hardly persistent enough to classify as a regu- 
 lar member of the Barrens. In the Charleston, West Virginia, region 
 a massive pebbly sandstone occurs not far from the horizon of the 
 Saltsburg rock, and the one which caps the hills at the mouth of the 
 Big Sandy River may be identical with the same bed. 
 
 THE CAMBRIDGE LIMESTONES. 
 
 At many localities in Ohio two dark fossiliferous limestones occur 
 only 20 to 30 feet apart, and Prof. Orton, director of the Ohio Geologi- 
 cal Survey, has named them respectively the Upper and Lower Cam- 
 bridge limestones. In Ohio these beds generally occur from 90 to 130 
 feet under the Crinoidal limestone and are always very fossiliferous. 
 
 In many regions of Pennsylvania two dark fossiliferous limestones 
 occur, which correspond to the two in Ohio, only there they are 60 to 
 70 feet apart, and the upper one 90 to 120 feet under the crinoidal bed, 
 while the lower one is 150 to 190 feet below the same horizon. 1 have 
 identified the two in Pennsylvania with the two in Ohio, and have also 
 adopted the Ohio names, since the Pennsylvania beds are known under 
 several names in different parts of the field, while the Ohio names are 
 now well established. The upper one is the lighter colored of the two, 
 and while generally fossiliferous, the fossils are not so abundant as in 
 the lower limestone. This upper one was termed the Pine Creek lime- 
 stone in my Report Q of the Pennsylvania Survey, while in Somerset 
 County it seems to be identical with the Coleman limestone of Platt. 
 
 At Morgantown, West Virginia (Section 42), this bed is dark, quite 
 fossiliferous, and lies 85£ feet below the Crinoidal limestone. 
 
 The term Black Fossiliferous limestone of the First Pennsylvania 
 Geological Survey Reports was probably applied quite as often to this 
 upper rock as to the lower one, since at times they very closely re- 
 semble each other, and contain practically the same fossils. 
 
 The interval separating the two limestones is generally shale in Ohio, 
 but in Pennsylvania it is sometimes a massive sandstone, and 60 to 90 
 feet thick. 
 
 The Lower Cambridge limestone is identical with the one termed 
 Brush Creek limestone by the writer in Report 'Q, Second Geological 
 Survey of Pennsylvania, but the geological horizon of that limestone 
 was there placed lower than it should have been by 50 to 60 feet, since 
 it was considered to belong between the two members of the Mahoning 
 
94 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65 . 
 
 sandstone, instead of above both members, and hence the term Brush 
 Greek limestone should be dropped from the nomenclature, and Lower 
 Cambridge substituted. This lower limestone is very fossil iferous, 
 often being a mere mass of Brachiopods and Lamellibranchs, of which 
 the most common are Chonetes mesoloba , Athyris subtilita , Pruductus 
 Nebracensis and a large Solenomya, together with Nautiliis occidentalis 
 and Orthoceras cribrosum. 
 
 This bed seems to be quite as persistent in Ohio as the Crinoidal 
 limestone, since it is present in almost every section at the proper 
 horizon, from Steubenville clear around to fronton, near which latter 
 poiut it is only 75 feet above the base of the Barrens. 
 
 In the hills at Catlettsburg, Kentucky, a dark fossiliferous limestone 
 occurs at 160 feet above the Upper Freeport coal, but this is probably 
 the Upper Cambridge, and the same limestone occurs in the summits 
 of the hills opposite Louisa, Kentucky, at 200 feet above the Upper 
 Freeport bed. It is barely possible, however, that this may be the 
 Lower Cambridge limestone, since the Barrens thicken very rapidly 
 southward from their northwestern outcrop. In the Berlin section, 
 (37), the Lower Cambridge limstone appears to be represented by the 
 Philson limestone of Platt. The “ calcareo- siliceous rock” of Hildreth, 
 in Ohio, appears to represent the same bed. 
 
 THE MASONTOWN COAL. 
 
 At an interval of 5 to 20 feet below the Lower Cambridge lime- 
 stone there occurs a coal bed which has quite a wide distribution. It 
 attains its best development in the region of Masontown, Preston 
 County, West Virginia, and it has been designated from that village. 
 It is there, and at many other points in the Preston basin, mined for 
 domestic purposes, being known as the u 4-foot” bed, and is a dry, 
 open-burning coal, highly prized for domestic fuel. It is everywhere 
 preferred to the Upper Freeport, which is accessible in the same 
 region. 
 
 This appears to be the same bed which the writer described in Re- 
 port Q, Second Geological Survey of Pennsylvania, under the n^ine of 
 Brush Creek coal, since a diamond drill hole has recently shown that 
 the Brush Creek bed lies 135 feet above the Upper Freeport coal instead 
 of 75, as formerly supposed, and hence it is deemed best to drop the 
 name Brush Creek altogether for both the coal and the limestone. 
 This Masontown coal is generally the first one above the top of the 
 Mahoning sandstone, and the interval separating it from the latter varies 
 from 5 to 50 feet. Very frequently the coal is only one-half to 1 foot 
 thick, and sometimes it is represented only by black slate. 
 
 Near Gallitzin, Pennsylvania, it is seen in a cut on the old Por- 
 tage Railroad, where it is only one-half foot thick, but it is overlaid by 
 3 to 4 feet of black slate. The coal is here 140 feet above the Upper 
 
WIUTK.J 
 
 THE BARREN MEASURES. 
 
 95 
 
 Freeport coal as measured in the McCoy shaft, which starts at the horn 
 zon of the Masontown bed. 
 
 This coal is reported as present at many localities in Ohio, though 
 there it seldom exceeds 2 feet in thickness. It is probably this bed 
 which has been opened near the summit of the hill opposite Louisa, 
 Kentucky, where it is 2 feet thiek and rather slaty. 
 
 In the Beliugton basin, Barbour County, West Virginia, this coal 
 attains a fine development and is often 4 to 5 feet thick with 6 inches 
 of bony coal near the center. 
 
 THE IRONDALE LIMESTONE AND ORE. 
 
 Directly under the Masontown coal there is occasionally found a bed 
 of huffish gray limestone, which at Irondale, Preston County, West 
 Virginia, and adjoining regions, is accompanied by a bed of iron ore 
 immediately under the limestone. 
 
 When the ore is present, however, the coal above is generally absent, 
 as is the case at Irondale and Gladeville, Preston County, where the ore 
 has been used to a considerable extent. It varies in thickness frotn 1 
 to 2 feet, and is rather siliceous, there being only about 38 per cent of 
 metallic iron in the ore. It comes 155 feet above the Upper Freeport 
 coal, and hence its horizon is assigned to that of the Masontown coal, 
 since the interval agrees, and then a similar limestone 3 feet thick is 
 seen under the coal at Albright and other localities in Preston County. 
 
 THE MAHONING SANDSTONE. 
 
 This is the lowest sandstone deposit of the Barren Measures, and al- 
 though at times consisting of one solid rock, yet it is generally complex. 
 The usual rule is for the mass to divide into two sandstones, an Upper 
 and Lower Mahoning, each 40 to 50 feet thick, with a shale interval 
 between containing a coal bed and limestone or iron ore, but sometimes 
 when the group reaches a great development, as on the Big Kanawha 
 (Section 49), it contains three coal beds, and as many sandstone divi- 
 sions. This is exceptional, however, the normal structure having only 
 two sandstones with one included coal, the whole series being 100 to 
 150 feet thick. 
 
 The wild scenery and poor soil of the lower portion of the Barrens 
 are largely due to these sandstones. Being frequently quite hard and 
 even pebbly, they cap the hills long after all the other members of the 
 Barrens above have disappeared, and they have thus protected the 
 underlying Lower Coal Measures over wide areas where the latter 
 would otherwise have been carried away by erosion. 
 
 In Wyoming County, West Virginia, they cap the summits of Guy- 
 ahdotte Mountain at an elevation of 3,000 feet above the sea. Much of 
 the Lower ( oal Measures between that mountain and the Great Ka- 
 nawha River would have been swept away but for this massive coping. 
 
 It is the same friendly cover that has preserved large areas of the 
 
96 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL 65 . 
 
 Coal Measures on the summits of the Alleghany Mountains, and in iso- 
 lated basins like Broad Top. The great tunnels on the Pennsylvania 
 and Baltimore and Ohio Railroads, Gallitzin and Kingwood respect- 
 ively, pass under domes of this sandstone group. Some portious of 
 this sandstone nearly always furnish good building rock, the Govern- 
 ment locks on the Great Kanawha being constructed of it. The same 
 stone is also largely quariied along the Ohio River hills in Beaver 
 County, Pennsylvania. 
 
 The Upper Mahoning is generally more massive than the Lower one, 
 and is the conglomeritic member, since it is often a mere mass of quartz 
 pebbles, having once been quarried for mill stones on Cheat River near 
 Morgantown. In the Great Kanawha region this rock is extremely 
 hard and siliceous, and at many points a mere bed of pebbles, some of 
 which are as large as an egg. 
 
 THE MAHONING COAL. 
 
 This is the coal bed which is so often bound up between the two 
 great divisions of the Mahoning sandstone. It was formerly called 
 the Brush Creek by the writer, but as the place of that coal was mis- 
 understood, it is thought best, as already stated, to drop the name en- 
 tirely, and replace it with the name Mahoning, since it comes in the 
 middle of the Mahoning sandstone. It is possible that the Gallitzin 
 coal of Platt in Cambria and Blair Counties may belong at this horizon, 
 but owing to the uncertainty connected therewith it has been deemed 
 best not to adopt that name. 
 
 This is a very widely distributed coal bed, and frequently attains 
 commercial importance. It is the coal No. 7 of the eastern Ohio series, 
 where it is 3 feet thick and very excellent fuel. It is mined at many 
 localities in Ohio, as well as in Pennsylvania. 
 
 On the Great Kanawha River, a few miles above Charleston, this bed 
 swells out to a thickness of 17 feet in the vicinity of Coalburg ; but 
 much of this is slate and bone, there being only 5 to 6 feet of good coal 
 in the bed. There is probably a considerable area of this coal of mer- 
 chantable thickness in the region southwest from the Great Kanawha, 
 since it is several feet thick along the summits of ridges in the Huff 
 Creek Mountains, at the southern line of Logan County, and the same 
 bed is 5 feet thick along the Tug branch of Big Saudy, and in the 
 Peach Orchard region of Kentucky, where it occurs 235 feet above the 
 Peach Orchard bed (Winnifrede). The coal is quite hard, and in many 
 places a “ block” coal through this southwestern region. The interval 
 of this bed above the base of the Barren Measures varies from 50 to 
 175 feet, this latter being the figure at Coalburg and Peach Orchard. 
 
 THE MAHONING LIMESTONE. 
 
 Occasionally a limestone comes into the series immediately under the 
 Mahoning coal. In Beaver County, Pennsylvania, it is often 5 to 8 feet 
 
WHITE.] 
 
 THE BARREN MEASURES. 
 
 97 
 
 thick, and is locally termed the “ Summit” limestone. It is not a per- 
 sistent bed, being much less so than the coal of the same name above, 
 and when present it is often impure and ferruginous. In fact it is occa- 
 sionally an iron ore, the Johnstown ore of Pennsylvania being identical 
 with this stratum. 
 
 THE UPPER AND MIDDLE CANNELTON COALS. 
 
 Along the Great Kanawha, where all of the measures have thickened 
 up so abnormally, two other coal beds make their appearance in the 
 Barren series below the Mahoning coal, and they have been termed the 
 Upper and Middle Cannelton, from a locality on the Kanawha where 
 both .are exposed. The former has there been mined for a long time in 
 the summit of the hills, where it furnishes 5 feet of excellent “block” 
 coal. It comes 90 feet above the base of the series, but the interval 
 constantly decreases northward, and at Charleston is only 40 to 50 
 feet. As this interval decreases the coal becomes inferior, until at 
 Charleston it is represented by some coaly streaks only, about the mid- 
 dle of the Lower Mahoning sandstone. 
 
 The Middle Cannelton coal never attains commercial value, and is 
 found only in the region of Cannelton and southward. It is slaty, 
 worthless, never more than 3 feet thick, and comes 20 to 25 feet above 
 the base of the Barrens. 
 
 The Lower Mahoning sandstone is generally of a bluish gray color, 
 quite homogeneous, and often an excellent building stone. Though 
 occasionally containing pebbles, it is much freer from them than the 
 Upper Mahoning. The thickness varies from 30 to 50 feet, except in 
 the Kanawha region, where it splits up into two or three divisions, and 
 is more than 100 feet thick. 
 
 The shales which separate the Upper and Lower Mahoning sand- 
 stones are sometimes red, or variegated, as in the Sewickley section 
 (34); and, occasionally, as in the vicinity of Tuunelton, Preston County, 
 West Virginia, good fire clay occurs at the horizon of the Mahoning 
 limestone. 
 
 Both members of the Mahoning sandstone are occasionally oil-pro- 
 ducing, but more generally the upper one, this being the main oil rock 
 at Bobtown, on Dunkard Creek, Greene Couuty, Pennsylvania, and 
 on Whitely Creek. It is known to the oil producers as the “Dunkard 
 sand,” and it is also oil-bearing in the Macksburg and other regions of 
 Ohio. 
 
 The shales which usually intervene between the base of the Mahon- 
 ing sandstone and the Upper Freeport coal often contain fossil Brach- 
 iopods and Lamellibrauchs, as well as the common coal measure plants. 
 They are quite variable in thickness, the Lower Mahoning sometimes 
 cutting out the shales entirely and resting on the Upper Freeport coal, 
 while again the shales may thicken up to 50 feet. 
 
 Bull. 65 7 
 
98 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65 . 
 
 THE KANAWHA BLACK FLINT. 
 
 In the midst of the shales at the base of the Barrens, and apparently 
 at the horizon which usually contains the marine fossils, there occurs 
 along the Great Kanawha River a peculiar deposit, known locally as 
 the u Black Flint.” It makes its appearance in the section first at 
 Charleston, and occurs from there southward along the river until the 
 Barrens disappear from the summit of Gauley Mountain, 50 miles dis- 
 tant. 
 
 The distribution of the flint appears to be confined to a belt along 
 the river 10 to 12 miles wide, since at 5 to 0 miles back on either side it 
 generally disappears from the section, so as to be no longer recogniza- 
 ble. It is not confined to the Kanawha region however, since the 
 deposit is visible near Clay Court House, on Elk River, and near the 
 California House, on the crest of the Burning Springs anticlinal, where 
 it crosses Hughes River at the corner of Wirt and Ritchie Counties. 
 The rock varies from 5 to 15 feet in thickness, and is usually of a dark 
 or bluish black color, though at the California House it is light colored. 
 Being almost indestructible by atmospheric agencies, it has played a 
 conspicuous part in shaping the topography in the Kanawha region, 
 since it protects the underlying beds from erosion. Through the agency 
 of heat and cold it finally breaks down into oblong and rudely rectang- 
 ular blocks which everywhere line the beds of streams and cover the 
 surface below the line of outcrop. The Indians manufactured arrow 
 heads and other implements fr.)m this material, so that pieces of it have 
 been found as far north as Pennsylvania. It is evidently a marine 
 deposit, since it is distinctly stratified, and specimens of Discina , Spi- 
 rifera , and Productus are common in the less siliceous layers. The flint 
 is evidently derived from the skeletons of diatoms aud protozoa, though 
 no microscopic examination has been made. 
 
 
CHAPTER V. 
 
 THE LOWER COAL MEASURES, OR ALLEGHANY RIVER SERIES. 
 
 THICKNESS, CHARACTER, AND EXTENT. 
 
 Below the Barren Measures or Elk River series there occurs a group 
 of rocks (No. XIII) which always holds valuable coal beds. From the 
 fact that they are finely exposed along the Alleghany River, they were 
 long ago called the Alleghany River series, and their geological posi- 
 tion in the general scale of the Carboniferous gave them the name 
 Lower Coal Measures. The discovery in recent years that the next 
 lower group of beds (the Pottsville Conglomerate) sometimes holds 
 workable coal, has been used as an argument by some geologists for 
 breaking up the old nomenclature and rearranging the Carboniferous 
 into new groups, but this nomenclature is so convenient, and expresses 
 the natural divisions of the rocks so well, that it would be very unwise 
 to make any such changes as have been proposed, since it would be of 
 no particular service and would only bring confusion to the minds of 
 many people interested in Carboniferous geology who are now thor- 
 oughly conversant with the old and tried nomenclature of Pennsylvania 
 and Virginia. Hence, while for strictly scientific purposes it may be 
 well to group the Carboniferous rocks on a wider basis as proposed in 
 a former part of this report, yet for every day field work in practical 
 geology, the old nomenclature can not be improved upon. 
 
 The Lower Coal Measures, as now limited, begin at the top with the 
 widely distributed and valuable Upper Freeport coal bed (a horizon 
 which is easily recognized anywhere by the field geologist) and extend 
 down through several beds of shale, limestone, coal, and sandstone till 
 a horizon is reached where a marked change in lithology takes place, 
 the sandrocks becoming harder, more massive, and often pebbly, accom- 
 panied with a corresponding change in the character of the imbedded 
 fossils. 
 
 The thickness of this series varies greatly in different portions of the 
 field, beiug not far from 300 feet in western Pennsylvania, and seldom 
 less than 250 feet anywhere in that State, except in the Broad Top 
 field. But westward through Ohio the thickness of these measures 
 declines until around the northwestern border of the field it is less than 
 200 feet. Southward from this region of Ohio, where the Lower Coal 
 Measures are thinnest, they thickeu up rapidly until on the Great Ka- 
 nawha River the series is 1,000 feet thick, and the same on the Guyan- 
 
 99 
 
100 THE NORTHERN BITUMINOUS COAL FIELD. [bull. 65. 
 
 dotte and Tug Rivers. Just where this great thickening up begins in 
 goingsouthwestward from the Pennsylvania line is not exactly known, 
 but there are good reasons for believing that much the greater portion 
 of it takes place beyond the Little Kanawha River. 
 
 The topography made by these rocks is generally very much the 
 same, except where the thickness is very great. It is nearly everywhere 
 characterized by a hilly country, terraced with a series of parallel 
 benches which, as Lesley long ago showed, mark the outcrops of the 
 several coal beds, since the soft rocks usually found with every coal 
 are more rapidly eroded than the harder ones above or below. These 
 coal benches are not confined to the topography of the Lower Coal 
 Measures, since they are due to a general law of erosion, but are only 
 more conspicuous in this series because the coal beds are more numer- 
 ous and closer together. 
 
 Through Pennsylvania, Ohio, and the northern half of West Vir- 
 ginia, with few exceptions, the hill slopes of these measures, while often 
 rather steep, are not too rugged for good arable and grazing lands, and 
 the soils are usually rich; but in the southwestern part of West Vir- 
 ginia, where these rocks have increased in thickness so largely, we find 
 a network of narrow ridges, generally capped with the Mahoning sand- 
 stone, from which the surface falls away at an angle of 25° to 40° to 
 the beds of the streams, 1,000 or more feet below, thus practically con- 
 fining the arable land to the narrow valleys, which are frequently 
 trenched into the top members of the next underlying or Potts ville 
 series of rocks. 
 
 It was formerly supposed that this series held valuable coal only in 
 a broad belt around the margins of the coal field, and that in the cen- 
 ter of the Appalachian basin, where these beds are buried under 1,500 
 to 2.000 feet of superincumbent strata, they contained no coals thick 
 enough to mine; but the recent drilling of many oil and gas wells over 
 the central portion of the field has proved the supposition to be un- 
 founded, for the drill has many times j)enetrated thick beds of coal in 
 this series at localities where they underlie the surface by an interval 
 of more than 1,500 feet. Hence, aside from local irregularities always 
 to be found in any coal field, there is no reason for believing that the 
 Lower Coal Measures do not contain one or more good coal beds under 
 nearly every portion of the Appalachian field, and where it would seem 
 to be otherwise the inference has been founded largely on defective 
 records of borings, in which no attention was given to the character of 
 the beds encountered unless they proved to be “ sands.” But while it 
 is true that recent drilling has shown valuable coal in this series along 
 the central portion of the trough where it was formerly supposed to be 
 absent, yet it is true as a general law that the coal beds of this series 
 are thicker and better and more numerous around the margins of the 
 Appalachian field than toward the center. This is illustrated by the 
 
GEOLOGICAL SURVE 
 
 LOWER COAL MEASURES, COALBURG, KANAWHA RIVER, WEST VIRGINIA. 
 

 
 
 fBE LIBRARY 
 Of THE 
 
 UHSVERSITY OF ILLINOIS 
 
WHITE.] THE LOWER COAL MEASURES. 101 
 
 distribution of the Clarion and Brookville beds, which are valuable 
 only around the margin of the coal area. 
 
 Owing to the geological position of the Lower Coal Measures, their 
 beds have a much wider spread and are accessible over a larger area 
 than those in the Upper Coal Measures, so that when in the distant 
 future the upper coals and the easily accessible areas of the lower ones 
 shall have been exhausted, there will still remain far down in the 
 trough of the Appalachian field a great wealth of fuel which can be 
 obtained by deep shafting. It is true that at many localities disclosed 
 by the drill only one good bed of coal has been found in this series 
 where it lies so deep beneath the surface, but that is also true of the 
 surface outcrops, and many, places can be found where not even one 
 good coal bed occurs in the surface section, and many others where 
 two are the exception. 
 
 The main strata of this series, which have been recognized and traced 
 over a wide area in the three States with which this report deals, have 
 received the following names in descending order: 
 
 Upper Freeport coal. 
 
 Upper Freeport limestone. 
 Upper Freeport sandstone. 
 Lower Freeport coal. 
 
 Lower Freeport limestone. 
 Lower Freeport sandstone. 
 Upper Kittanning coal. 
 Johnstown (Cement) limestone. 
 Middle Kittanning coal. 
 
 Lower Kittanning coal. 
 Lower Kittanning fire clay. 
 Lower Kittanning sandstone. 
 Buhrstone iron ore. 
 Ferriferous limestone. 
 Putnam Hill limestone. 
 Clarion coal. 
 
 Brookville coal. 
 
 Other beds have been named in this series which have a local dis- 
 tribution, but those given above are the main ones which can be traced 
 and identified over wide areas. 
 
 Prof. Orton, director of the Ohio Geological Survey, has shown that 
 all of the main beds of the Pennsylvania Lower Coal Measures can be 
 followed and identified entirely across the Ohio coal field to where they 
 enter Kentucky ; and the writer has recently shown (The Virgiuias, 
 1885) that they also stretch unbroken around the southeastern margin 
 of the Appalachian field, from the Pennsylvania line down through 
 West Virginia to the Great Kanawha, and on across the Guyandotte 
 to the Big Sandy, so that the identifications of the main beds of coal, 
 limestone, and sandstone of the Lower Coal Measures have now been 
 carried from Pennsylvania to the Kentucky line, on both sides of the 
 Appalachian field. 
 
 As illustrations of these measures, in most of the important coal re- 
 gions of the area in question, we shall now present a number of vertical 
 sections. The identifications of the several beds in these sections have 
 been made with all the care and light at present attainable, and while 
 it is not claimed that they are final in all cases and free from error, yet 
 they express the best efforts of the writer, and it is confidently believed 
 
102 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 that their publication will serve to stimulate a more careful study of 
 the general stratigraphy by field geologists and those interested in 
 mining enterprises, so that finally whatever of error may be embodied 
 in these identifications will be discovered and eliminated. It is certain 
 that the first effort to harmonize the stratigraphy over such a large 
 area will be somewhat provisional, and hence the writer not only ex- 
 pects, but welcomes, the kindly criticism of his brother geologists, 
 knowing that all will be pleased when the true order and succession of 
 these beds are definitely determined in the several important regions 
 of the Appalachian field. 
 
 In some cases, like that at Blossburg, where it has been impossible 
 to identify the main coal beds with any degree of certainty, the writer 
 has given only the local names for the beds, leaving the reader to draw 
 his own conclusions from the general structure of the section 5 but 
 there are very few cases where some one of the seams in a given section 
 can not be reasonably determined. 
 
 We shall begin these illustrations of the Lower Goal Measures at the 
 most northern point of the Appalachian Basin, and proceed south- 
 westward through the field. 
 
 Section at Blossburg , Pennsylvania . — The structure of the Lower Coal 
 Measures at the northern en$ of the Appalachian basin is given as 
 follows (Fig. 50) for the Blossburg region, Tioga County, Pennsylvania, 
 by the First Geological Survey of Pennsylvania, Final Report, Yol. II, 
 page 520 : 
 
 Blossburg , Tioga County , Pennsylvania. 
 
 ■HiJgpWj 
 
 r2TT~' ~ 
 
 <*>• 
 
 20 ' 
 
 !?} ,oV 
 uV 
 3‘s" 
 
 Fig. 50.— Section at 
 Blossburg, Pa. 
 
 2710 
 
 aV-* 
 
 30' 
 
 47lo" 
 
 [See map, B w.J 
 
 Ft. in. Ft. in. 
 
 1. Coal, “Eock vein” 3 6 
 
 2. Concealed T ... 22 
 
 3. Coal, “Seymour" 5 
 
 4. Slate and sandstone 10 
 
 5. Concealed 10 > 47 10 
 
 6. Sandstone, pebbly, with thin coal near top 27 10 ' 
 
 7. Coal, “Dirty vein” .iJi.. 3 6 
 
 8. Slate and sandstone 30 
 
 9. Coal. 1 6 
 
 10. Fireclay 3 
 
 11. Slate 20 
 
 ( Coal 3' 6” ) 
 
 12. Coal, “Bloss vein”. < Fire clay. 5' 0" > 10 6 
 
 ( Coal 2' V'S 
 
 13. Argillaceous sandstone, with two thin coals 13 6 
 
 14. Coal, “ Bear Creek ” 3 6 
 
 15. Sandstone. 
 
 163 10 
 
 Total. 
 
 The “ Bloss vein” seems to be identical with the Lower Kittanning 
 
 bed of the Alleghany River, while the “Rock vein” and “Seymour” 
 are possibly identical with the Upper and Lower Freeport beds, respect- 
 ively. This would make Nos. 7 and 9 the Upper and Middle Kittan- 
 ning. 
 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 103 
 
 Section at Fall Brook , Pennsylvania . — At Fall Brook, 8 miles north- 
 east from Blossburg, and the most northern development in the Appala- 
 chian coal field, the structure of the Lower Coal Measures is given as 
 follows (Fig. 51) by Mr. Franklin Platt, in Beport G, pages 166, 169, 
 Second Geological Survey of Pennsylvania : 
 
 Fall Brook, Tioga County, Pennsylvania. 
 
 [See map, B x.] 
 
 Ft. in. 
 
 2 6 
 
 1. Coal, “Seymour” 
 
 2. Bough, sandy fire clay 2 
 
 3. Sandstone, massive, pebbly 50 
 
 Coal. 
 
 4. Coal < Sandstone, thin bedded 
 
 ( Coal 
 
 5. Eire clay 
 
 6. Sandstone 
 
 7. Slate 
 
 [Coal.. 
 
 Slate . 
 
 Dirty vein ” { Coal. 
 
 1 ' 8 " 
 3 ' 0 " 
 O' 7" 
 
 8. Coal, 
 
 
 mp 
 
 Fig. 51. — Section 
 at Fall Brook , 
 Pa. 
 
 1' 3" ] 
 
 4' 0" | 
 
 , 1' 2" > 
 
 Slate . 0' 3" | 
 
 [Coal.. 0' 10 " ) 
 
 9. Bough, hard fire clay , 2 
 
 10. Gray shaly rock 20 
 
 11. Fire clay, with kidney ore at bottom - 2 
 
 12. Sandstone, light gray 9 
 
 13. Clay slate 5 
 
 14. Coal, “Bloss vein” 4 
 
 15. Fire clay, pure 3 
 
 16. Sandy slate, some sandy layers 16 
 
 17. Coal and slate, “ Bear Creek ” 1 
 
 18. Sandy clay 4 
 
 19. Sandstone. 
 
 Total 
 
 146 
 
 Section near Karthaus, Pennsylvania . — About 65 miles southwest of 
 Blossburg, in the northeastern corner of Clearfield County, Penn- 
 sylvania, the following section (Fig. 52) of the Lower Coal Measures 
 is reported from the vicinity of Karthaus, by H. D. Kogers, in the First 
 Geological Survey of Pennsylvania : 
 
 near Karthaus, 
 Pa. 
 
 Karthaus, Clearfield County, Pennsylvania. 
 
 [See map, E t.] 
 
 Coal, Upper Freeport 
 
 Fire clay 
 
 Sandstone, brown 
 
 Coal 
 
 Fire clay 
 
 Limestone, siliceous 
 
 Shale 
 
 Sandstone, brown 
 
 Coal, Lower Freeport 
 
 Slate 
 
 Sandstone, gray, Freeport 
 
 Coal, Upper Kittanniug 
 
 Shale, containing iron ore 
 
 Coal. Middle Kittanning 
 
 Sandstone and slate 
 
 ( Coal. 1' 0"l 
 
 Coal, Lower Kittanning < Slate O' 3" > 
 
 (Coal 2' 6" ) 
 
 Fire clay 
 
 Sandstone, brown 
 
 Coal, Clarion 
 
 Fire clay, ferruginous 
 
 Shales, containing iron ore band 
 
 Shales and slates 
 
 Coal, Brookville 
 
 No. XII Conglomerate. 
 
 Total 
 
 Ft. in. 
 6 
 
 2 6 
 45 
 
 0 ie 
 2 
 
 3 6 
 
 1 
 
 26 
 
 3 
 
 1 6 
 37 
 
 3 2 
 
 11 
 1 
 
 21 
 
 3 9 
 
 2 6 
 35 
 
 1 6 
 
 3 
 
 11 9 
 
 22 
 1 
 
 245 
 
104 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 Tbull. 65. 
 
 Section in Horton Township, Hlk County , Pennsylvania. — Horton Town- 
 ship, Elk County, Pennsylvania, lies on the borders of Clearfield and 
 Jefferson Counties, 30 miles west from Karthaus and 
 about 80 miles distant west-southwest from the Bloss- 
 burg region. In this township Mr. C. A. Ashburner 
 finds the following section (Fig. 53) for the Lower Coal 
 Measures, Eeport BE, page 227 : 
 
 Horton Township, Elk County, Pennsylvania. 
 
 [See map, Dq.j 
 
 
 Fig. 53. — Section in 
 Elk County, Pa. 
 
 ( Coal 3 
 
 1 . Coal, Upper Freeport n Fire clay and shale. . . 10 
 
 ( Coal 3 
 
 2. Fire clay and sandstone 
 
 3. Limestone, Upper Freeport 
 
 4. Slaty sandstone 
 
 5. Coal, Middle Freeport 
 
 6 . Soft gray slates 
 
 t Cannel 2' 
 
 7. Coal, Lower Freeport < Slate 16' 
 
 ( Coal 3' 
 
 8 . Sandstone - 
 
 9. Limestone. Lower Freeport 
 
 10. Flaggy sandstone and slates 
 
 11. Coal, Upper Kittanning 
 
 12 . Fire clay and slate 
 
 13. Limestone, Johnstown Cement 
 
 14. Concealed 
 
 35. Coal, Middle Kittanning 
 
 16. Black slate 
 
 17. Coal, Lower Kittanning 
 
 18. Shale and sandstone, occasional coal streak 
 
 19. Limestone, Ferriferous 
 
 20. Shale and slate 
 
 21. Coal, Clarion 
 
 22. Massive sandstone, top of XU. 
 
 Total 
 
 Feet. 
 
 16 
 
 :!■ 
 
 327 
 
 Section near Broclcwayville , Pennsylvania . — Snyder Township, Jeffer- 
 son County, adjoins Horton, and there, near Brockwayville, Mr. Wm. 
 
 G. Platt reports the following structure (Fig. 54) for the 
 Lower Coal Measures, Eeport H 6 , pages 186, 187 : 
 
 2V 
 
 
 
 Fig. 54. — Section 
 near Brockway- 
 ville, Pa. 
 
 Brockwayville, Jefferson County, Pennsylvania. 
 
 [See map, D q.] 
 
 Ft. in. 
 
 1. Coal, Upper Freeport ~ 3 
 
 2. Clay, impure 3 
 
 3. Limestone, Upper Freeport 5 
 
 4. Concealed 24 
 
 5. Sandstone, thin-bedded 5 
 
 6. Shales and slates 6 
 
 7. Coal, Lower Freeport ' 3 6 
 
 8. Clay, impure 5 
 
 9. Limestone, Lower Freeport 2 6 
 
 10. Concealed 18 
 
 12. Sandstone 15 
 
 13. Slates 5 
 
 14. Coal, Upper Kittanning 3 6 
 
 35. Clay shales 12 
 
 16. Limestone, Johnstown Cement 2 
 
 17. Concealed, shales (?) 40 
 
 38. Coal, Middle Kittanning 2 
 
 19. Concealed, sandstone at base 45 
 
 20. Coal, Lower Kittanning 2 1 6 
 
 21. Shales 35 
 
 22. Iron ore, Buhrstone 6 
 
 23. Limestone, Ferriferous 5 
 
 24. Sandstone and shales 20 
 
 25. Concealed 15 
 
 26. Coal, Clarion 3 
 
 27. Shales 10 
 
 28. Sandstone, massive, top of XII. 
 
 Total 
 
 290 
 
WHITE.! 
 
 THE LOWER COAL MEASURES. 
 
 105 
 
 Section in Clarion County , Pennsylvania . — Clarion County lies next 
 west from Jefferson, and Mr. H. Martyn Chance gives in Report VV", 
 page 32, Second Geological Survey of Pennsylvania, the 
 following as the general structure of the Lower Coal 
 Measures in that county (Fig. 55) : 
 
 
 
 Fig. 55. — Section 
 
 in Clarion Co., 
 
 Clarion County, Pennsylvania. 
 
 [See map, E o.J 
 
 1. Coal, Upper Freeport 
 
 2. Fireclay. 
 
 3. Limestone, Upper Freeport 
 
 4. Sliale, with ore 
 
 5. Sandstone 
 
 6. Shale 
 
 7. Coal, Lower Freeport 
 
 8. Fire clay 
 
 9. Limestone, Lower Freeport 
 
 10. Sandstone and shales 
 
 11. Shale 
 
 12. Coal, Upper Kittanning 
 
 13. Fire clay or shale 
 
 14. Limestone, Johnstown Cement bed 
 
 15. Shalv measures 
 
 16. Coalj Middle Kittanning 
 
 17. Fireclay 
 
 18. Shale and sandstone 
 
 19. Coal, Lower Kittanning 
 
 20. Sandstone and shale, with ore 
 
 21. Ore, Buhrstone 
 
 22. Limestone, Ferriferous 
 
 23. Shale 
 
 C Coal . . . ..I 2' ) 
 
 24. Clarion coal < Slaty sbalo. .... 25' > 
 
 ( Coai y.. 3L> 
 
 25. Fireclay 
 
 26. Shale and sandstone 
 
 27. Coal, Brookville 
 
 28. Fire clay 
 
 29. Massive sandstone, XII. 
 
 Ft 
 
 Pa. 
 
 Total - 335 
 
 * Section at Miller's Eddy, Clarion County , Pennsylvania . — 
 zs r y r The following section (Fig. 56), made by Mr. John Hag- 
 
 * gerty, M. E., of Brady’s Bend, Pennsylvania, represents 
 the Lower Coal Measure structure at Miller’s Eddy, near 
 the mouth of the Clarion River (YV, p. 123) : 
 
 
 to/ 
 
 IB'S- 
 
 Miller's Eddy , Clarion County, Pennsylvania. 
 
 [See map, En.] 
 
 2. Interval. 
 
 3. Iron ore. 
 
 6. Interval . . . 
 
 7. Sandstone. 
 
 9. Coal, Lower Kittanning. 
 10. Interval 
 
 12. Limestone, Ferriferous. 
 
 13. Shales 
 
 14. Sandstone 
 
 Fig. 56. — Section 
 at Miller’s Eddy, 
 
 Pa. 
 
 16. Blue shales 
 
 17. Sandstone, massive. 
 
 Total 312 
 
 Ft. in. 
 
 3 
 
 
 28 
 
 3 
 
 2 
 
 
 103 
 
 
 1 
 
 6 
 
 20 
 
 
 30 
 
 
 16 
 
 6 
 
 3 
 
 6 
 
 10 
 
 
 19 
 
 10 
 
 9 
 
 
 6 
 
 
 28 
 
 6 
 
 2 
 
 4 
 
 29 
 
 
 312 
 
 5 
 
106 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section at East Brady , Clarion County , Pennsylvania . — Mr. Haggerty 
 also leveled another section of these measures at East Brady, in the 
 southwestern corner of Clarion County, which is given as 
 follows (Fig. 57) in Report YV, p. 77 : 
 
 East Brady , Clarion County , Pennsylvania . 
 
 [See map, F n.] 
 
 Ft. in. 
 
 Coal. Upper Freeport 2 
 
 Concealed and sandstone -. 108 
 
 Coal, Upper Kittanning 1 5 
 
 Sandstone 9 
 
 Interval 57 0 
 
 Coal, Lower Kittanning 3 6 
 
 Shale, with sandstone 40 6 
 
 Limestone, Ferriferous 10 
 
 Interval 22 2 
 
 Coal, Clarion 
 
 Sandstone 
 
 Coal, thin, Brookville. 
 Sandstone, No. XII. 
 
 Fig. 57. — Section 
 at East Brady, 
 
 Total. 
 
 279 
 
 Section near New Bethlehem , Pennsylvania . — Mr. Chance gives the 
 following (Fig. 58) as the structure of the Lower Coal Measures in the 
 vicinity of New Bethlehem, on the Red Bank River, in 
 southeastern Clarion County, YY, p. 88 : 
 
 
 Fig. 58.— Section 
 near New Beth- 
 lehem, Pa. 
 
 Near New Bethlehem, Clarion County, Pennsylvania . 
 
 [See map, F o.] 
 
 1. Coal, Upper Freeport 
 
 2. Fireclay 
 
 3. Sandy shale and sandstone 
 
 4. Coal, Lower Freeport - 
 
 5. Fire clay 
 
 6. Concealed, sandstone, and shale 
 
 7. Coal, Upper Kittanning 
 
 8. Fire clay 
 
 9. Shale 
 
 10. Coal, Middle Kittanning (?) 
 
 11. Fire clay 
 
 12. Concealed 
 
 13. Ore, Buhrstone 
 
 14. Limestone, Ferriferous 
 
 15. Concealed 
 
 16. Sandstone, top of XII. 
 
 Ft. 
 
 5 
 
 3 
 
 42 
 7 
 3 
 
 65 
 
 3 
 
 4 
 
 43 
 2 
 
 3 
 
 60 
 
 1 
 
 4 
 
 50 
 
 Total 295 
 
WHITE.) 
 
 THE LOWER COAL MEASURES. 
 
 107 
 
 Section in Brady Township , Butler County , Pennsylvania. — In the 
 northwestern portion of Butler County (Brady Township), Mr. Chance 
 gives, in Beport V, the following section (Fig. 59) for 
 the Lower Coal Measures down to and including the 
 Ferriferous limestone, and the portion below that is 
 added from an exposure in an adjoining township : 
 
 60 ’ 
 
 Brady Township, Butler County. 
 
 [See map, F L] 
 
 Ft. Ft. 
 
 55 ' 
 
 1. Coal, Upper Freeport 
 
 2. Fire clay 
 
 3. Shale and sandstone 
 
 4. Coal, Lower Freeport 
 
 5. Concealed, and massive sandstone 
 
 6. Massive sandstone 
 
 7. Coal, Upper Kittanning 
 
 8. Concealed, and shale 
 
 9. Coal, Middle Kittanning (?) 
 
 10. Concealed 
 
 11. Iron ore thin l 
 
 12. Concealed -• 55 j 
 
 13. Limestone, Ferriferous 
 
 14. Coal, Scrubgrass 
 
 15. Shales 
 
 1G. Coal, Brookville 
 
 m. 
 
 G 
 
 45, 
 
 15 i 
 
 10 ) 
 
 Total 
 
 GO 
 
 3 
 
 55 
 
 3 
 
 65 
 
 15 
 
 1 
 
 328 
 
 Section near Ore Hill Furnace , Armstrong County , 
 
 fig. 59. Section in But- Pennsylvania. — In the vicinity of Ore Hill Furnace, 
 
 ier county, Pa. Armstrong County, Pennsylvania, 3 miles below the 
 mouth of the Mahoning Fiver, the writer found the fol- 
 ( lowing succession (Fig. 60) : 
 
 Ore Hill Furnace, Armstrong County, Pennsylvania. 
 
 [See map, G o.] 
 
 1. Coal, Upper Freeport 
 
 2. Fire clay with iron ore 
 
 3. Flaggy sandstone and shales 
 
 4. Bit uminous shales 
 
 5. Coal, blossom. Lower Freeport 
 
 6. Fire clay and limestones, Lower Freeport 
 
 7. Flaggy sandstone and dark shales 
 
 8. Limestone, gray, Johnstown Cement 
 
 9. Concealed and sandstone 
 
 10. Coal, Middle Kittanning 
 
 11. Fire clay 
 
 12. Sandy shale 
 
 (Coal V 0' 
 
 13. Coal, Lower Kittanning (Shale 4' 0" 
 
 ( Coal O' 6" 
 
 14. Fire clay 
 
 15. Shales, brown, sandy 
 
 16. Iron ore, Buhrstone 
 
 17. Limestone, Ferriferous 
 
 Fig. 60.— Section nea r 18. Concealed and shales to top of No. XII sandstone in Al- 
 
 Ore Hill Furnace* leghany River 
 
 Ft. 
 
 Ft. in. 
 
 
 2 6 
 
 8) 
 
 
 20 V 
 
 33 
 
 5) 
 
 
 30 \ 
 
 35 
 
 
 1 
 
 
 50 
 
 J" s 
 
 Armstrong County* 
 
 Pa. 
 
 Total 
 
 247 
 
 This section exhibits a rapid thinning away of the whole column, 
 but principally in that part of it between the Upper Freeport and the 
 Upper Kittanning coals. 
 
108 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section near Centerville , Pennsylvania . — Five miles northeast from Ore 
 Hill Furnace, the following succession (Fig. 61) is reported from the 
 vicinity of Centerville by Mr. Win. G. Platt, in Eeport 
 H 5 , Second Geological Survey of Pennsylvania, pages 
 
 163, 164. 
 
 Centerville , Armstrong County, Pennsylvania. 
 
 [See map, G- o.J 
 
 Ft. 
 
 
 15 ) 
 
 65 
 
 Fig. 61.— Section 
 
 near Centerville, 
 Pa. 
 
 1. Coal, Upper Freeport 
 
 2. Clay shales, with iron ore 
 
 3. Limestone, Freeport u > 
 
 4. Concealed 15 ) 
 
 5. Coal, Lower Freeport : . . . 
 
 6. Concealed 
 
 7. Iron ore, siliceous 
 
 8. Sandstone 
 
 9. Coal, blossom 
 
 10. Concealed 
 
 11. Coal, Upper Kittanning 
 
 12. Concealed 
 
 13. Coal, Middle Kittanning 
 
 14. Concealed 
 
 15. Iron ore, Buhrstone 
 
 16. Limestone, Ferriferous 
 
 17. Concealed 
 
 18. Cannel slate (Clarion coal) .. 
 
 19. Concealed 
 
 20. Black slate (Brookville coal). 
 
 21. Top of No. XII conglomerate. 
 
 Total 298 2 
 
 Section at Putnfyville, Pennsylvania. — Five miles east 
 of Centerville is the village of Putney ville, and from 
 this vicinity Mr. Wm. G. Platt reports the following 
 
 Ft. 
 
 in. 
 
 3 
 
 10 
 
 35 
 
 
 3 
 
 6 
 
 37 
 
 
 46 
 
 
 1 
 
 
 27 
 
 
 1 
 
 6 
 
 65 
 
 
 0 
 
 4 
 
 8 
 
 
 30 
 
 
 40 
 
 
 298 
 
 2 
 
 section (Fig. 62) of the series H 5 , p. 150: 
 
 
 rtf 
 
 42 r 
 
 SX* 
 
 Putneyville, Armstrong County, Pennsylvania, 
 
 [See map, G o.] 
 
 1. Coal. Upper Freeport 
 
 6. Coal, Lower Freeport 
 
 7. Slate 
 
 10. Concealed 
 
 12. Coal, blossom, Upper Kittanning . . . 
 
 13. Limestone, Johnstown Cement bed. 
 
 14. Clay 
 
 17. Coal, Middle Kittanning 
 
 18. Concealed 
 
 19. Slates, with sandstone layers. 
 
 20. Coal, Lower Kittanning 
 
 21. Fire clay, impure 
 
 24. Limestone, Ferriferous 
 
 25. Sandstone, flaggy 
 
 26. Black slates 
 
 27. Cannel slate (Clarion coal) 
 
 28. Concealed 
 
 29. Brookville coal. 
 
 30. Top of No. XII, conglomerate. 
 
 Ft. in. 
 
 
 Ft. 
 
 in. 
 
 
 
 
 4 
 
 G 
 
 12 
 
 
 ) 
 
 
 
 5 
 
 10 
 
 
 1 
 
 > 
 
 j 
 
 42 
 
 
 15 
 
 
 3 
 
 
 1 
 
 6 
 
 [ 
 
 
 
 0 
 
 3 
 
 
 
 2 
 
 
 53 
 
 9 
 
 30 
 
 
 
 
 
 20 
 
 
 J 
 
 4 
 
 
 3 
 
 
 
 
 
 15 
 
 
 
 58 
 
 
 40 
 
 
 > 
 
 1 
 
 8 
 
 30 
 
 20 
 
 
 } 
 
 50 
 
 
 
 
 
 2 
 
 
 6 
 
 
 J 
 
 
 
 20 
 
 
 5 
 
 26 
 
 4 
 
 0 
 
 4 
 
 5 
 
 
 
 Fig. 62. — Section at 
 Putneyville, Pa. 
 
 Total 
 
 314 3 
 

 t«.y- 
 
 WHITE.} 
 
 THE LOWER COAL MEASURES. 
 
 109 
 
 Section near Kittanning , Pennsylvania . — In the vicinity of Kittan- 
 ning, Pennsylvania, the succession of the Lower Coal Measures is as 
 follows (Fig. 63) : 
 
 Vicinity of Kittanning, Pennsylvania. 
 
 [See map, G n.j 
 
 Ft. in. 
 
 1. Coal, Upper Freeport 
 
 2. Shales, and concealed 
 
 3. Coal, Lower Freeport 
 
 4. Concealed, and massive sandstone 35 
 
 5. Shales and sandstone 40 
 
 6. Coal, slate in center. Middle Kittanning 
 
 7. Fire clay 4 
 
 8. Sandy shales 6 
 
 9. Fire clay 3 
 
 10. Flaggy sandstone 17 
 
 11. Shales, dark, sandy, with iron ore. 
 
 ('Coal... 
 i Slate . . 
 
 12. Coal, Lower Kittanning . . ^ Coal . . . 
 
 40 
 
 1' 
 
 10" } 
 
 O' 
 
 2 " | 
 
 0' 
 
 8" > 
 
 .0' 
 
 1" 1 
 
 .0' 
 
 6"J 
 
 L Coal 
 
 13. Fire clay - 5 
 
 14. Sandstone and sandy shales 
 
 15. Shales, with iron ore 
 
 16. Iron ore, Buhrstone 
 
 17. Limestone, Ferriferous 11 
 
 18. Sandy shales 15 
 
 19. Coal 
 
 20. Sandy shales and sandstone 
 
 21. Coal, Clarion 
 
 22. Concealed, to top of Xo. XII sandstone 
 
 Ft. in. 
 
 4 
 
 35 
 
 2 
 
 75 
 
 1 6 
 
 Fig. 63. — Section near 
 Kittanning, Pa. 
 
 Total . 
 
 D 
 
 40 
 
 } 
 
 > 50 
 
 5 
 
 
 ► 
 
 0 
 
 6 > 
 
 
 11 
 
 6 
 
 > 27 
 
 15 
 
 
 0 
 
 
 
 21 
 
 
 
 1 
 
 
 
 25 
 
 
 
 315 
 
 Section 5 miles south of Kittanning, Pennsylvania. — About 5 miles 
 south of Kittanning and 1 mile below the mouth of Crooked Creek a 
 very important exposure may be seen on the left bluff of the Allegheny 
 Eiver, since it gives in a clear manner the relations of the upper mem- 
 bers of the Lower Coal Measures. The section there (Fig. 64) was 
 carefully leveled by the writer, and reads as follows : 
 
 Five miles helow Kittanning. 
 
 [See map, G n. ] 
 
 1. Coal, Upper Freeport, blossom 
 
 2. Fireclay 
 
 3. Sandstone 
 
 4. Fire clay and shales 
 
 5. Concealed . 
 
 6. Limestone, Upper Freeport 
 
 7. Concealed 
 
 8. Shales, bluish 
 
 t Coal .... 0' 2" I 
 
 9. Coal, Lb wer Freeport. .. < Slate r 8" t 
 
 t Coal 1' 8") 
 
 10. Fire clay and shales - 
 
 11. Sandstone, massivo, pebbly, Frbepmt 
 
 12. Coal, Upper Kit lunn in g .->.;!■> 
 
 13. Shales, daik 
 
 14. Coal, slate in center, Middle Kittanuing 
 
 15. Limestone, sandy 
 
 16. Fire clay 
 
 17. Sandstone, flaggy 
 
 18. Fireclay 
 
 19. Sandstone, flaggy 
 
 20. Shales, dark 
 
 Ft. in. 
 
 2 6 ) 
 2 6 
 
 5 
 
 10 
 
 35 
 
 20 
 
 10 
 
 45 
 
 Ft. in. 
 
 80 
 
 3 6 
 
 55 
 
 0 6 
 20 
 
 1 6 
 1 6 
 
 3 
 
 3 - 
 
 5 
 8 
 10 
 
 Total 
 
 191 
 
110 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section at Logansport , Pennsylvania , — The last section gets its special 
 significance when compared with another one, obtained 2 miles below, 
 on the right bank of the Alleghany River, and opposite the town of 
 Logansport. The section there (Fig. 65) gives the following structure; 
 
 Logansport, Armstrong County, Pennsylvania. 
 
 [See map, Gr n.] 
 
 Ft. 
 
 1. Coal, Upper Freeport. 
 
 2. Fire clay 
 
 f Impure limestone. 2' ) 
 
 I Limy shales 4' 
 
 I Limestone, good V 
 
 3. Limestone, Upper Freeport Shales V 
 
 I Limestone, “glassy layer” 2' 
 
 , Limy shales 2' 
 
 [ Limestone, good 2' 
 
 70 
 
 51 ’ 
 
 Fig. 65. — Section at Lo- 
 gansport, Pa. 
 
 ' 8 ” ) 
 
 ' 2"L. 
 ' 6 ” ) 
 
 f Coal 
 
 V 
 
 1" 
 
 j Slate 
 
 
 l" 
 
 17. Coal, Lower Kittanning . . <{ Coal 
 
 V 
 
 1" 
 
 | Slate 
 
 0' 
 
 V 
 
 1 Coal 
 
 V 
 
 2" 
 
 Ft. in. 
 3 
 
 4 ) 
 
 14 )• 28 
 
 18. Concealed to river level 
 
 19. To base of Lower Coal Measures, about 
 
 4. Shales and fire clay 10 J 
 
 fCoal 2' 0”) 
 
 5. Coal, Lower Freeport < Fire clay, impure. 2' 4'' > .. 
 
 ( Coal 4' 8" ) 
 
 6. Concealed 11 » 
 
 7. Very massive, grayish white, pebbly sandstone, Freeport 70 > 
 
 8. Coal, ltl>per Kittanning. ...L. ...;v 
 
 9. Dark gray shales v 
 
 ( Coal 0 
 
 10. Coal, Middle Kittanning. \ Slate 0 
 
 , f Coal 0 
 
 11. Fireclay ?.* 
 
 12. Limestone 
 
 13. Fire clay, with limestone nodules in top . 
 
 14. Sandstone, shaly 
 
 15. Concealed (shales) 1 
 
 16. Blue shales 
 
 7 
 
 15 
 20 J 
 
 81 
 
 0 8 
 20 
 
 1 4 
 
 y 52 
 
 3 6 
 
 Total 298 6 
 
 Here we find a ferruginous limestone making its appearance under 
 what the section shows to be the Middle Kittanuing coal, and it is pos- 
 sible that this same bed may have occasionally been identified with 
 the Johnstown Cement limestone in this portion of Pennsylvania, 
 which would be erroneous, since that bed belongs under the little coal, 
 No. 8 of the section, while the Johnstown Cement bed, as correlated by 
 Messrs. Platt and others, comes just under the Upper Kittanuing coal. 
 
 The section also exhibits the great variations that may take place 
 in the thickness of the intervals between important coal beds, that 
 between the two Freeports being here reduced to only 28 feet. 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 Ill 
 
 Section at Freeport, Pennsylvania . — Freeport, on the Alleghany River, 
 at the southern point of Armstrong County and 7 miles southwest of 
 Logansport, is a classic locality for the upper portion of the Lower Coal 
 Measures, and the following section (Fig. 66), taken there, is given 
 for the purpose of illustrating the relations of the Upper and Lower 
 Freeport coals at this typical locality : 
 
 Freeport , Pennsylvania. 
 [See map, G n.] 
 
 Ft. in. 
 
 [Coal 2' 8 "l 
 
 1 Slate, gray O' 1^" ( 
 
 1. Coal, Upper Freeport { Coal O' J> 
 
 1 Slate, dark gray 0? 0-£" i 
 
 ( Coal, sulphurous O' 5 " J 
 
 2. Fire clay 
 
 3. Limestone, Upper Freeport 3 
 
 4. Sandy shales 20 
 
 5. Coal, Middle Freeport . . Jr.C V'-i 2 
 
 6. Sandy shales and sandstone 39 
 
 [ Cannel slate... 5' 0"] 
 
 ^ j Slaty coal 4' 
 
 7. Coal, Lower Froeport <J Fire clay with } 
 
 ^ " | limestone 2' 6" | 
 
 (Slaty coal 2' 6"j 
 
 8. Fire clay and shales 2 
 
 g ! 
 
 
 Fig. 66.— Section at 
 Freeport, Pa. 
 
 g-2 ^ 10. Coaly slate, Upper Kittannin 
 j r § (11. Sandstone, gray, massive 15 
 
 12. Coal, Middle Kittanning 
 
 13. Fire clay, with limestonenodules in upper half.. 
 
 Total 
 
 Ft. in. 
 3 
 
 14 
 
 64 
 
 155 3J 
 
 This section shows that there is a third Freeport coal, coming nearly 
 midway between the upper and lower ones, at this, their typical 
 locality, a fact that has been frequently overlooked by geologists, and 
 that has led to error in identifications. This Middle Freeport coal, as 
 
 I have termed it, is not persistent; but the fact that there is such a 
 bed in the series occasionally should lead to careful scrutiny of this 
 portion of the column of rocks before positive identification of the 
 Lower Freeport coal. 
 
 This latter bed, No. 7, also has elements of possible confusion in its 
 structure here at its type locality, since, as may be seen from the sec- 
 tion, it is a double bed, made so by 2J feet of fire clay, in which a nod- 
 ular limestone occurs. It is possible that these parting rocks may 
 expand to several feet in some regions, and thus give two Lower 
 Freeport coals, as indeed they are known to do. 
 
 I have included No. 11 as a part of the Freeport sandstone, since at 
 one locality the coal bed No. 10 thins out entirely and lets Nos. 9 and 
 
 II unite into one solid sandstone; but it is possible that No. 9 alone 
 should be included under the name Freeport sandstone, as originally 
 intended by Rogers. 
 
112 
 
 THE NORTHERN BIT OMINOUS COAL FIELD, 
 
 [BULL. 65, 
 
 Section near mouth of Beaver River , Pennsylvania. —In the region 
 about the month of the Beaver River, the Lower Goal 
 Measures thicken up to a considerable extent, through 
 the local expansion of some members, as shown by 
 the following (Fig. 67) section of the structure there: 
 
 vX\\\%%vJv: tst 
 
 4d 
 
 Near mouth of Beaver River , Beaver County, Pennsylvania. 
 
 87' 
 
 iiifliiiilil iN 
 
 42 ' 
 
 80 ' 
 
 i81 f 
 
 [See map, Gk.] 
 
 Ft. 
 
 1. Coal, Upper Freeport 
 
 2. Fireclay... 4 
 
 3. Limestone, Upper Freeport i 2 
 
 4. Shales, sandy 55 
 
 5. Coal, Lower Freeport 1 
 
 6. Shales, sandy 12 
 
 7. Sandstone, massive, Freeport 75 
 
 8. Coal, Middle Kittanning 
 
 9. Fire clay 3 
 
 10. Shales, sandy, dark 40 
 
 11. Coal, Lower Kittanning ®i 
 
 12. Fire clay : 8 
 
 13. Sandstone, flaggy and massive 42 
 
 14. Shales, sandy . . 1 r 30 
 
 15. Limestone, Ferriferous 
 
 16. Black fossiliferous shales 12 
 
 17. Fireclay 8 
 
 18. Sandy shales 10 
 
 19. Fire clay, non-plastic 3 
 
 20. Sandstone, flaggy 23 
 
 21. Shales, sandy 25 
 
 22. Coal, Brookville 
 
 23. Fire clay 
 
 24. Massive sandstone, No. XII. 
 
 Ft. in. 
 3 
 
 61 
 
 81 
 
 Total 
 
 369 
 
 Section at Sewicldey , Pennsylvania. — At Sewickley, 
 Alleghany County, Pennsylvania, a test hole for coal 
 F moutiT of C B°e n a v G © r was bored by Mr. Cochran Fleming, through whose 
 Kiver, Pa. courtesy the writer had the opportunity of measuring 
 
 the carefully preserved cores from the diamond drill, which gave this 
 structure (Fig. 68) for the rocks of the Lower Coal 
 Measures there : 
 
 a 
 
 
 
 nil 
 His 
 
 Sewickley, Alleghany County, Pennsylvania. 
 
 [See map, H 1.] 
 
 Ft. in. 
 
 7S* 
 
 Fjg. 68.— Section at Se 
 wiekley, Fa, 
 
 1. Coal, Upper Freeport 
 
 2. Fire clay 15 
 
 3. Shales, blue, sandy 9 
 
 4. Sandstone 0 
 
 5. Fireclay 3 
 
 6. Sandstone 1 
 
 7. Shales 16 
 
 8. Dark slate 6 
 
 9. Coal, slaty, Lower Freeport 
 
 10. Fire clay, good 1 
 
 11. Fire clay, sandy 3 
 
 12. Gray, micaceous sandstone $ ° n6 "•*«/ <u// 
 
 in thin layers Freeport \^ dstobe % 
 
 13. Coal, Upper Kittanuing 
 
 14. Sandstone 16 
 
 15. tire clay (Middle Kittanning coal horizon) 8 
 
 16. Shales, dark, in terst ratified with fire clav 48 
 
 ( Coal ..1' 4' 
 
 17. Coal, Lower Kittanning < Slate 0' 1 
 
 (Coal 0 
 
 18. Fire clay, good 
 
 19. Shales, blue 
 
 20. Interval to top of No. XII, estimated 
 
 Ft. in. 
 
 L 
 
 
 i 
 
 39 6J f 
 
 Total . 
 
 l 3 
 
 44 Si 
 
 0 4i 
 
 73 
 
 8 
 
 16 10 
 75 
 
 £75 8 
 
WHITE. J 
 
 THE LOWER COAL MEASURES. 
 
 113 
 
 Section at Washington , Pennsylvania . — At Washington, Pennsylvania, 
 the top of this series is 1,000 feet below the surface, and Prof. Linton, 
 of Washington and Jefferson College, gives the follow- 
 ing (Fig. 69) as the structure of its rocks according 
 to the record of the Thayer oil well, the drillings from 
 which he very carefully studied (Geological Survey of 
 Pennsylvania, 1886, pp. 764, 765) : 
 
 Under Washington, Pennsylvania. 
 
 fSee map, J k.] 
 
 1. Upner Freeport coal— absent 
 
 2. Dark shale with limestone at bottom, Upper Freeport 
 
 3. Sandstone, dark 
 
 4. Sandstone, white 
 
 5. Sandstone, dark, with limestone 
 
 6. Sandstone, hard 
 
 7. Shale, dark 
 
 8. Shale, variegated with dark lime 
 
 9. Limestone, Johnstown Cement - - ^ fight’ * g/j 
 
 10. Shale, dark, slaty 
 
 11. Shale and coal, Middle Kittanning 
 
 12. Shale, slate and shells 
 
 13. Sandstone, grayish 
 
 14. Shale, gray 
 
 15. Sandstone, grayish, shaly 
 
 16. Shale and shells 
 
 Total 
 
 Ft. 
 
 Ft. 
 
 12 ) 
 
 
 36 > 
 
 64 
 
 16 S 
 
 4 
 
 19 ) 
 
 28 > 
 
 55 
 
 8 > 
 
 11 
 
 
 30 
 
 30 ] 
 26 [ 
 
 6 
 
 U > 
 
 115 
 
 29 | 
 
 
 19 J 
 
 
 
 285 
 
 it would 
 
 Fig 69.— Section under 
 Washington, Pa. 
 
 Here there is only one coal present in the series and 
 appear to be the Middle Kittanning. 
 
 Section near Carpenters Station , W estmor eland County , Pennsylvania . — 
 Kear the main line of the Pennsylvania Eailroad, in the vicinity of Car- 
 penter’s Station, Westmoreland County, Pennsylvania, a 
 well was drilled for gas by Mr. E. M. Hukill, who thus 
 (Fig. 70) reports the structure of the Lower Coal Meas- 
 ures, as published in Geological Survey of Pennsylvania, 
 1886, p. 726: 
 
 |»r 
 
 i 
 
 44 6 
 
 Near Carpenter’s Station , Westmoreland County, Pennsylvania. 
 
 [See map, In.] 
 
 7. Sandstone, Freeport 
 
 1. Coal, Upper Freeport 
 
 2. Fireclay (shales) 
 
 3. Coal, Lower Freeport 
 
 4. Fire clay 
 
 5. Sandstone, gray 
 
 6. Slate 
 
 C Sandstono, hard . 
 < Sandstone, soft . 
 ( Sandstone, hard. 
 
 8. Slate 
 
 9. Sandstono 
 
 10. Slate and shells 
 
 11. Slate, black 
 
 18. Coal, Clarion or Lower Kittanning 
 
 19. Fire clay 
 
 20. Shale and shells 
 
 70.— Section 21. Sandstone, top of XII. 
 
 6 ') 
 44 ' [ 
 13 ' > 
 
 Fig. 
 
 near Canjen ter’s 
 Station, Pa. 
 
 Total 
 
 Bull. 65 
 
 Ft. 
 
 Ft. 
 
 
 2 
 
 
 65 
 
 
 2 
 
 9 1 
 
 j 
 
 30 
 
 
 5 1 
 
 r- 107 
 
 63 J 
 
 1 
 
 15 1 
 
 5 ! 
 
 45 ! 
 
 1 
 
 > 92 
 
 27 J 
 
 7 
 
 
 12 
 
 
 16 
 
 
 303 
 
114 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section under Murray sville , Pennsylvania. — At Murraysville, West- 
 moreland County, Pennsylvania, in the celebrated natural gas region, 
 the top of the Lower Coal Measures lies 60 to 75 feet below the surface, 
 and the structure of the series is thus given (Fig. 71) 
 by Mr. Doubleday, from the records of a gas well on 
 the Remaley farm, Geological Survey of Pennsylvania, 
 1SSG, p. 721 : 
 
 
 
 Under Murraysville , Westmoreland County, Pennsylvania. 
 
 [See map, I n.] 
 
 Ft. 
 
 ( Coal V 
 
 1. Coal, Upper Freeport < Slate 5' 1 
 
 (Coal 4'! 
 
 2. Slate 
 
 3. Coal, slate in center. 
 
 4. Slate 
 
 Fig. 71.— Section 
 under Murrays- 
 ville, Pa. 
 
 5. . Sandstone 
 
 6. Slate 
 
 7. Slate and shells 
 
 8. Massive sandstone, top of XII. 
 
 * I 
 
 Ft 
 
 10 
 
 135 
 
 Total. 
 
 236 
 
 Section on Beaver Run , Westmoreland County , Pennsylvania. — About 
 9 miles northeast of Murraysville a well was drilled on Beaver Run, 
 beginning only 4 feet below the level of the Upper Freeport coal. The 
 record (Fig. 72) of this well, as given by Mr. J. A. Mebaffey, shows 
 the following structure there (Pennsylvania Geological Survey, 1886, 
 p. 728) : 
 
 
 16’ 
 
 
 20' 
 
 S’ 
 
 6' 
 
 If 
 
 st 
 
 
 
 
 
 
 si 
 
 §^rm 
 
 
 
 % 
 
 
 
 
 
 
 
 
 ar 
 
 If 
 
 
 ■SS7: 3=== 
 
 
 
 s’J 
 
 Beaver Bun, Westmoreland County, Pennsylvania. 
 
 8S’ 
 
 Fig. 72. — Section on 
 Beaver Run, Pa. 
 
 [See map, H n.J 
 
 1. Coal, Upper Freeport 
 
 2. Concealed 
 
 3. Black slate 
 
 4. Limestone 
 
 5. Coal, Lower Freeport . 
 
 6. Fire clay 
 
 7. Shell, hard 
 
 8. Shale, soft 
 
 9. Slate, black 
 
 10. Shale, soft 
 
 11. Slate, black 
 
 12. Coaly slate, Upper Kittanning 
 
 13. Sandstone 
 
 14. Slate, black 
 
 15. Sandstone, gray 
 
 16. Slate, black 
 
 17. Sandstone 
 
 18. Coal, Lower Kittanning 
 
 19. Fireclay 
 
 20. Iron ore 
 
 21. Shales, soft 
 
 22. Fireclay 
 
 23. Pebbly srndstone, top of XII. 
 
 Ft 
 
 Ft. in. 
 3 6 
 
 5 J 
 
 Total . 
 
 77 
 
 85 
 
 4 
 
 ‘25 
 
 6 
 
 2 
 
 18 
 
 276 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 115 
 
 Section near Richmond , Pennsylvania . — In the northern portion of 
 Indiana County, Pennsylvania, in the vicinity of Richmond village, 
 the Lower Coal Measures exhibit the following struc- 
 ture (Fig. 73) according to Mr. Wm.G-. Platt, H 4 . p. 266: 
 
 Near Richmond, Indiana County , Pennsylvania. 
 
 Ft. 
 
 
 12 j 
 
 TV ■ 
 
 '«* L 
 
 |^= ===='5==-.^^ 
 
 
 ==~-===r;-== ' 
 
 20 1 
 
 =• ==L-=.r= 
 
 J 
 
 
 I5 r 
 
 
 Ilf 
 
 
 io' : 
 
 
 K' 
 
 
 s* 
 
 
 to' 
 
 
 Z5' * 
 
 
 : T 
 
 i- 
 
 
 45’ 
 
 
 
 
 atfl 
 
 
 io' J 
 
 
 4' 
 
 
 
 
 20 
 
 ===■^1=-= 
 
 r 
 
 Er = =;= 
 
 
 
 30* 
 
 
 
 
 5. Coal, Lower Freeport . . . 
 
 [See map, F p.] 
 
 1. Coal, Upper Freeport 
 
 2. Clay - 
 
 3. Limestone 
 
 4. Shales and thin sandstone 
 
 Coal... thin ) 
 Shales. 15' > .. 
 Coal... thin ) 
 
 6. Concealed 
 
 7. Sandstone 
 
 8. Clay slate 
 
 9. Coal, Upper Kittanning.. 
 
 10. Concealed - 
 
 11. Shales 
 
 12. Sandstone 
 
 13. Slate and shales 
 
 14. Coal, MiddleKittanning 
 
 15. Interval 
 
 16. Coal. Lower Kittanning 
 
 17. Interval 
 
 18. Shales 
 
 19. Limestone, Ferriferous 
 
 20. Shales and slates 
 
 21. Coal, Clarion 
 
 22. Shales 
 
 23. Sandstone, massive, top of XII. 
 
 Total 
 
 10 
 
 10 
 
 5 
 
 5 ) 
 
 10 1 
 25 f 
 
 5 J 
 
 Ft. in. 
 
 42 
 
 15 
 
 25 
 
 281 6 
 
 Fig. 73. — Section near 
 Richmond, Pa. 
 
 Section near Lockport and Bolivar , Indiana County , 
 Pennsylvania . — In the vicinity of Bolivar and Lockport 
 just east of the Chestnut Ridge anticlinal, Mr. Wm. G. Platt finds the 
 following succession (Fig. 74) for these measures as given in H 4 , p. 65: 
 
 Near Lockport and Bolivar, Indiana County, Pennsylvania. 
 
 [See map, I p.] 
 
 1. Coal, Upper Freeport 8 
 
 2. Clay shales 6 ] 
 
 3. Shales, with ore masses 3 
 
 4. Sandstone and sandy shales 10 [ 
 
 5. Fire clay, good 3 } 52 
 
 6. Limestone, impure, Upper Freeport 8 
 
 7. Thin bedded sandstone 7 | 
 
 8. Clay slates and shales 15 j 
 
 9. Coal, Lower Freeport 2 9 
 
 10. Clay, impure 3 ] 
 
 11. Limestone, Lower Freeport 5 j 
 
 12. Clay shales 10 
 
 13. Sandstone 7 
 
 14. Sandy fire clay 3 
 
 15. Slates and shales 20 
 
 16. Sandstone 10 
 
 17. Grayish slates % . . . 6 
 
 i i , j mu ii . i mi 18. Coai, Upper Kittanning » 1 10 
 
 J ] 9 . Fire clay, impure 6 ] 
 
 20. Limestone, Johnstown cement 3 I 
 
 ., . ,i 21. l)ark slates and shales 20 
 
 t P 36 22. Sandy shales with ore nodules. 20 
 
 " * ~ 23. Carbonate iron ore band 0 
 
 24. Black slates 10 
 
 25. Coal, Middle Kittanning 
 
 26. Slates 8 
 
 27. Shales 10 
 
 28. Black slate and shale 30 
 
 I 29. Coal, Lower Kittanning 
 
 ' 30. Clay 5 
 
 31. Sandstone 10 
 
 32. Shales and clay slates 13 
 
 f Coal thin 1 
 
 33. Clarion coal < Sandstone.. 5' > 6 
 
 ( Coal 1') 
 
 34. Fire clay 2 
 
 35. Shales 10 
 
 Fig. 74. — Section near 36. Sandstono, heavy, compact. 
 
 Lockport and Boii- 
 
 var, Pa. Total 2881 
 
 64 
 
 59 
 
 48 
 
 28 
 
116 
 
 THE NORTHERN BITUMINOUS COAL FIElD, 
 
 [bull. 65. 
 
 Section near Lauglilinstoicn , Pennsylvania. — In the vicinity of Laugh- 
 linstown, Westmoreland County, and 10 miles south from Bolivar, Dr. 
 Jno. J. Stevenson (KKK, p. 135) reports the Lower Coal Measures with 
 the following structure (Fig. 75) : 
 
 Laurel Bun, Ligonier Township , Westmoreland County, Pennsyl- 
 vania. 
 
 [See map, J p.] Ft. in. Ft. in. 
 
 
 Z-- 
 
 
 
 
 zsS 
 
 
 k' 
 
 Hill 
 
 mu 
 
 mu 
 
 i 
 
 ro' 
 
 
 a 
 
 S' 
 
 
 gH i^p 
 
 30' 
 
 
 
 
 *5' 
 
 
 za' 
 
 » 
 
 
 33. 
 
 iiiia 
 
 20' 
 
 
 s' 
 
 g' 
 
 
 Zh‘ 
 
 Fig. 75.— Section on 
 Laurel Eun, Pa. 
 
 1. Coal, Upper Freeport 
 
 2. Clay 6 
 
 3. Fire clay, non-plastic * 2 
 
 4. Sandstone 1 
 
 5. Concealed 11 
 
 6. Sandstone 1 
 
 7. Concealed 29 
 
 8. Shale 12 
 
 9. Coal, Lower Freeport 
 
 10. Shales 10 
 
 11. Concealed - 8 
 
 f Coal V 6") 
 
 12. Coal, Upper Kittanning < Sbaly sandstone 5' 0" s 
 
 (Coal 0' l"i 
 
 13. Shale 1 
 
 14. Limestone, Johnstown ^ g^™j® stone ^ ^ 
 
 Cement ( Limestone’ II !*. 1 1! V.V 0") 
 
 15. Shale 30 
 
 16. Coal, Middle Kittanning 
 
 17. Concealed 25 
 
 18. Sandstone 25 
 
 19. Shale 1 
 
 f Coal P 10" 1 
 
 | Clay O' 2" | 
 
 20. Coal, Lower Kittanning <( Coal F 0" )- 
 
 i Coal, slaty 0' 6" j 
 
 • [Carbonaceous shale .. V 8"J 
 
 21. Clay 
 
 22. Massive sandstone, coarse 
 
 23. Shale 
 
 24. Iron ore 
 
 25. Shale 
 
 26. Coal, Clarion 
 
 27. Shale 
 
 28. Ton of No. XIL 
 
 > 
 
 6 $ 
 
 Total 
 
 62 
 
 42 6 
 
 3 6 
 
 51 6 
 
 5 2 
 
 295 9 
 
 Section on Cucumber Bun , Stewart Township , Fayette Comity, Pennsyl- 
 vania. — Id this same basin (Ligonier) and on southwest- 
 ward near the Youghiogheny Biver, in Fayette County, 
 the Lower Coal Measures exhibit the following structure 
 (Fig. 76) on Cucumber Bun, as reported by Stevenson 
 (KKK, p. 89) : 
 
 Cucumber Bun, Stewart Township , Fayette County, Pennsylvania. 
 
 Ft. Ft. in. 
 
 [See map, K n.] 
 
 1. Coal, Upper Freeport 
 
 2. Clay 
 
 3. Limestone, Freeport 
 
 4. Fire clay, Bolivar, and shale 
 
 5. Shale, sandy 
 
 6. Coal, Lower Freeport (?) 
 
 7. Shale, sandy 
 
 ( Coal 2' 
 
 8. Coal, Upper Kittanning(?) < Clav O' 4 
 
 (Coal 3' 4" 
 
 9. Clay 
 
 l\ 
 
 44 
 
 
 10. Sandstone, Freeport(?). 
 ' * itly 
 
 11. Concealed (mostly sandstone) .. 
 
 12. Coal, Middle Kittanning 
 
 13. Sandstone 
 
 14. Concealed 
 
 15. Coal, Lower Kittanning 
 
 16. Concealed 
 
 17. Coal, Clarion orBrookvillo 
 
 18. Shah and clay 
 
 Fig. 76. — Section on 19. Sandstone, massive, top of XII. 
 
 Cucumber Eun, Fay- 
 ette County, Pa. ‘ Total 
 
 l\ 
 
 0 ) 
 
 0 8 
 30 
 
 5 11 
 83 
 
 blossom 
 
 35 
 
 blossom 
 
 60 
 
 2 3 
 
 10 
 
 273 10 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 117 
 
 Section at ffewburg, West Virginia . — Newburg, on the Baltimore and 
 Ohio Railroad, in Preston County, West Virginia, is situated at the 
 center of the same coal basin as Bolivar, Ligouier, etc., and there a 
 deep shaft reveals the following structure (Fig. 77) for the Lower Coal 
 Measures : 
 
 Shaft at Newhurg , Preston County , West Virginia. 
 
 [See map, O m.] 
 
 Ft. in. 
 
 1. Coal, Upper Freeport j CoS and slate.": 2' 4" } 
 
 2. Shales 8 
 
 3. Sandstone 18 
 
 4. Limestone, Upper Freeport 8 
 
 5. Shales 6 
 
 6. Iron ore 1 
 
 7. Shales . 4 
 
 8. Fire clay (horizon of Lower Freeport coal) 
 
 9. Shales, gray 14 
 
 10. Shale, dark 11 
 
 11. Shale, gray 9 
 
 12. Sandstone, Freeport 74 
 
 (Coal VO"] 
 
 13. Coal Tipper and Middle J % gill. 
 
 Kittanning ] Fire c i ay *. 2 ' 0" | 
 
 [Coal, good. 2' 0" ) 
 
 14. Fire clay and shales with iron ore nodules 
 
 Coal 0' 10" 1 
 
 Shale, gray O' 10" I 
 
 Coal O' 6" I 
 
 15. Coal, Lower Kittanning <( Coal, bony O' 3" > .. 
 
 1 Coal, main bench. 4' 6" 
 
 I Black slate 0' 6" 
 
 [Coal 2' 0". 
 
 16. Sandstone and shale 
 
 17. Pebbly sandstone, top of XII. 
 
 Ft. in. 
 5 4 
 
 45 
 
 Fig. 77 — Section at 
 Newburg, W. Va. 
 
 Total. 
 
 108 
 
 7 3 
 
 15 
 
 9 5 
 
 38 
 
 230 
 
 Here the Upper Freeport coal lies 150 feet below drainage and 700 
 feet below the tops of the immediate hills. 
 
 No. 13 appears to represent both the Upper and Middle Kittanning 
 coal beds, which are brought practically together, and also very close 
 to the Lower Kittanning bed by the thinning away of intervening 
 rocks. 
 
 The interval under the Lower Kittanning bed here is revealed by a 
 diamond drill hole which was put down 150 feet below the latter 
 stratum. 
 
 The Lower Freeport coal is not present, but its horizon is clearly 
 indicated by the bed of fire clay, No. 8, at 45 feet under the Upper 
 Freeport coal. 
 
 The Freeport sandstone, No. 12, has a large development, and where 
 it comes to the surface, 4 miles above Newburg, is nearly 100 feet 
 
 thick. 
 
118 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 fBULL. 65. 
 
 Section at Johnstown , Pennsylvania. — Johnstown, Pennsylvania, lies 
 just east of the Laurel Hill anticline, and the Lower Coal Measures 
 have there been splendidly exposed through the mining operations 
 of the Cambria Iron Company. The following section (Fig. 78) of the 
 rocks in that region is given by the chief engineer of the Cambria 
 Company, Mr. John Fulton (H 3 , pp. 308, 309) : 
 
 Vicinity of Johnstown, Cambria County, Pennsylvania. 
 
 [See map, I q.] 
 
 Coal, Upper Freeport. 
 Fire 
 
 clay. 
 
 Ft. 
 
 1 
 
 Shales 5 
 
 Sandstone 10 
 
 Shales 5 
 
 6. Kidney ore '. 0 
 
 7. Shales 15 
 
 8. Sandstone i 15 
 
 9. Shales 3 
 
 10. Coal, Lower Freeport 
 
 11. Shale 0 
 
 12. Limestone, Lower Freeport 3 
 
 13. Iron-stained shales 17 
 
 14. Sandstone, gray, micaceous 21 
 
 15. Slates 4 
 
 16. Coal, Upper Kittanning 
 
 17. Fireclay 0 
 
 18. Limestone, Johnstown Cement 5 
 
 19. Fire clay, impure 7 
 
 § 20. Slates, with iron ore 8 
 
 21. Slate 8 
 
 22. Black slates, with iron ore — It 
 
 (Coal 0' 3") 
 
 23. Coal, Middle Kittanning < Slate 1' 0" > 
 
 (Coal 0' 3 ") 
 
 24 % Thin black slates 13 
 
 25. Coal r 0 
 
 26. Fire clay 4 
 
 27. Sandstone, gray 13 
 
 28. Sandstone, wavy, gray 4 
 
 29. Iron-stained slates 6 
 
 30. Coal, Lower Kit tanning 
 
 31. Fire clay.. 3 
 
 32. Gray slates and shales 21 
 
 33. Massive black shales : 15 
 
 34. Gray sandstone 5 
 
 35. Massive black slate 5 
 
 36. Coal, thin 
 
 37. Black slates i 
 
 38. Gray sandstone 4 
 
 39. Thin gray slates 6 
 
 54.1&" 
 
 45V 
 
 
 4hV 
 
 ( Coal.. 
 
 40. Coal, Clarion Slate . 
 
 ( Coal.. 
 
 4' 6") 
 0 ' 6 " } 
 
 1 ' 10 " ) 
 
 EHE 26 
 
 41. Fireclay 
 
 42. Gray slates 
 
 43. White massive sandstoue, top of XII. 
 
 10 
 
 Ft. in. 
 3 0 
 
 54 10 
 
 2 6 
 
 45 6 
 
 39 9 
 
 1 6 
 
 40 9, 
 
 3 6 
 
 V 60 0 
 
 6 10 
 
 Fig. 78.— Section near 
 Johnstown, Pa. 
 
 Total. 
 
 3 0 
 
 28 0 
 
 292 8 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 119 
 
 Section at Gonemaugh , near Johnstown , Pennsylvania , — The writer 
 compiled a section of the Lower Coal Measures atConemaugh and else- 
 where in the vicinity of Johnstown, which differs only 
 in minor details from that of Mr. Fulton. It reads as 
 follows (Fig. 79) : 
 
 nm 
 
 3 r 6f 
 
 46' 
 
 40' 
 
 Is- 
 
 Fig. 79. — Section at 
 Conemaugh, Pa. 
 
 1. Coal, Upper Freeport 
 
 2. Fire clay »nd sandy .shales 
 
 3. Coal, Lower Freeport 
 
 4. Shales and sandy beds 
 
 5. Sandstone, massive 
 
 6. Coal, Upper Kittanning . . . 
 
 7. Shale 
 
 Near Johnstown , Pennsylvania. 
 
 [See map, I q.] 
 
 8. Limestone, Johnstown 
 
 Limestone 2' 6" 
 
 Shale and iron ore.l' 6" 
 
 9. 
 
 Cement (Limestone 4' 
 
 Dark sandy shales with iron ore 33 
 
 Coal and slate.. O' 6" 
 
 Slate 0' 6" 
 
 Slaty coal O' 10'' 
 
 Ft. in. 
 
 10. Coal, Middle Kittanning. 
 
 11. Shales, drab 
 
 12. Coal 
 
 13. Impure fire clay 
 
 14. Sandstone, gray micaceo 
 
 15. Sandy shales 
 
 16. Coal, Lower Kittanuing 
 
 17. Shales, sandy 
 
 18. Coal, Clariqn 
 
 19. Fire clay 
 
 20. Concealed and shales... 
 
 21. Top of xn. 
 
 Ft. in. 
 3 6 
 
 40 
 
 0 7 
 
 20 
 40 
 
 3 
 
 > 44 
 
 1 10 
 
 . 15 
 . 1 
 
 1 
 
 5 
 
 [ ,71 
 
 . 45 
 
 1 
 
 . 5 
 
 J 
 
 3 
 
 30 
 
 5 
 
 5 
 
 
 15 
 
 Total . 
 
 281 11 
 
 Section in Jackson Township , Cambria County , Pennsylvania. — In Jack- 
 son Township, Cambria County, 8 miles northeast of Johnstown, a 
 well was once drilled for oil, and I obtained from the con- 
 tractor the following record (Fig. 80) of the strata repre- 
 senting the Lower Coal Measures. It is chiefly important 
 as giving the total thickness of the series in a vertical 
 measurement: 
 
 Jackson Township, Cambria County , Pennsylvania. 
 
 [See map, I q.J 
 
 
 Ft. in. 
 
 1. Coal, Upper Freeport 3 
 
 2. Fire clay and slate 6 
 
 3. Sandstone, gray 44 
 
 4. Slate, drab 2 
 
 5. Coal, Lower Freeport 4 
 
 6. Fire clay and limestone 6 
 
 7. “Soapstone” (shale) 56 
 
 8. Sandstone, gray 36 
 
 9. Coal and slate, Lower Kittanning 6 
 
 ]0. Sandstone, gray 48 
 
 11. Shale 3 
 
 12. Coal, Clarion 6 
 
 13. Fire clay 3 
 
 14. Slate, gray 55 
 
 Fig. 80. — Section 15. Hard sandstone, top of XII. 
 
 in Jackson Town- 
 
 ship, Cambria 
 County, Pa. 
 
 
 55’ 
 
 Total 279 
 
120 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [hull. 65. 
 
 Section on Berts Greek , Cambria County , Pennsylvania. — ]^ear tbe 
 eastern border of Cambria County, along the waters of Ben’s Creek, in 
 Washington Township, the following section (Fig. 81) is reported by 
 Mr. Franklin Platt (H 2 , p. 48) : 
 
 Berts Creek, Cambria County, Pennsylvania. 
 
 [See map, I q.] 
 
 1. Coal, Upper Freeport 
 
 2. Fire clay 
 
 3. Black slates and shales 
 
 4. Limestone, Upper Freeport 
 
 5. Interval 
 
 6. Sandstone 
 
 7. Coal, Lower Freeport. 
 
 (Coal O' 2"1 
 
 J Sandstone 2' 0" ( 
 
 ) Fire clay and shale... 6' 0" 
 
 (Coal 2' 0"J 
 
 8. Fire clay 
 
 9. Limestone, Lower Freeport 
 
 10. Shales, iron-bearing 
 
 11. Coal, smnt 
 
 12. Fire clay, shales, with ore balls. 
 
 13. Coal, smut 
 
 14. Fire clay 
 
 15. Slates anil shales 
 
 16. Black slates 
 
 17. Coal, Upper Kittanning 
 
 18. Fire clay 
 
 Fig. 81.— Section on Ben’s 
 Creek, Cambria County, 
 
 Pa. 
 
 19. Drab shales 
 
 20. Sandstone, fine grained 
 
 2L Black slate 
 
 22. Coal, slaty, Middle Kittanning. 
 
 23. Fire clay 
 
 24. Sandstone 
 
 25. Fire clay, shale 
 
 26. Black slate 
 
 27. Coal, Lower Kittanning 
 
 28. Sandstone and shale 
 
 29. Coal. Clarion 
 
 30. Fire clay 
 
 31. Sandstone 
 
 32. Dove-colored shale, with ore — 
 
 33. Sandstone 
 
 34. Fire clay, shale 
 
 35. Coal, Brookville 
 
 36. Fire clay 
 
 37. Concealed 
 
 38. Top of XII. 
 
 Total 
 
 Ft. in. Ft. in. 
 
 4 4 
 
 6 
 
 15 
 
 15 
 
 12 
 
 \ 55 
 
 J 
 
 10 2 
 
 2 1 
 
 2 6 
 
 15 
 
 0 2 
 
 i 
 
 5 ^ 
 
 0 3 
 
 1 # 
 
 38 11 
 
 7 
 
 56 
 
 9 
 
 2 
 
 5 1 
 
 10 J. 20 
 
 5 J 
 
 3 
 
 18 
 
 5 
 
 5 1 
 
 0 10 | 
 
 10 j> 20 10 
 
 1 8 
 
 25 
 
 263 
 
 2 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 121 
 
 Section near Stoyestmcn , Pennsylvania . — In the vicinity of Stoyes- 
 town, on Stony Creek, Somerset County, Pennsylvania, near the center 
 
 11 “' 
 
 
 fi5 
 
 Fig. 82. — Section near 
 Stoyestown, Pa. 
 
 of the basin between the Viaduct and Negro Mountain 
 anticlines, the series exhibits the following structure 
 (Fig. 82) according to Mr. Franklin Platt (H 3 , p. 129) : 
 
 Stoyestoivn, Somerset County , Pennsylvania. 
 
 [See map, J q.] 
 
 1. Coal, Upper Freeport .. 
 
 2. Interval 
 
 3. Black slates 
 
 4. Coal, Lower Freeport 
 
 5. Fireclay 
 
 6. Limestone, Lower Freeport 
 
 7. Interval 
 
 8. Sandstone, massive 
 
 9. Black slates 
 
 10. Coal, Upper Kittanning 
 
 11 . Black .slate 
 
 12. Limestone, Johnstown Cement 
 
 13. Fireclay 
 
 14. Interval 
 
 15. Black slates 
 
 16. Coal, Clarion 
 
 17. Interval, concealed 
 
 18. Top of No. XII. 
 
 Total 
 
 Coal 3' > 
 
 Shale 8' > 
 
 Coal ... 3' ) 
 
 Ft. in. Ft. in. 
 
 14 
 
 3 
 
 2 
 
 7 
 
 30 
 
 8 
 
 0 
 
 7 
 
 ? 
 
 85 
 
 3 
 
 70 
 
 0 
 
 G 
 
 272 6 
 
 Section at Pinkerton Point , Pennsylvania. — On the Castleman River 
 at Pinkerton Point, in the southern portion of Somerset County, a very 
 complete section of the Lower Coal Measures was obtained by Mr. 
 Franklin Platt along the Baltimore and Ohio Bailroad, near Shoo Fly 
 Tunnel, and is reported as follows (Fig. 83) (EL 3 , pp. 202, 203) : 
 
 H 
 
 
 Pinlcei'ton Point, Somerset County, Pennsylvania. 
 
 [See map, L o.] 
 
 Fig. 83.— Section at 
 Pinkerton Point, 
 Somerset County, 
 Pa. 
 
 Upper Freeport Coal (absent) ■ 
 
 f Coal 2' 3 
 
 < Shale and fire clay 2' 0 
 
 Coal, Upper Kittannin ^ 
 
 ( Coal 1 
 
 Limestone, Johnstown Cement 
 
 Black slate 
 
 Coal, Middle Kittanning 
 
 3" ) 
 
 Coal. 
 
 Coal, Lower kittanning 
 Fire clay 
 
 Coal, Clarion 
 
 Fire clay 
 
 Sandstone 
 
 Slates, dark colored 
 
 Massive sandstone, top of No. XII. 
 
 Total 
 
 Ft. 
 
 in. 
 
 Ft. 
 
 2 
 
 
 
 65 
 
 
 77 
 
 10 
 
 s 
 
 5 
 
 6 
 
 ) 
 
 
 1.9 
 
 8 
 
 { 
 
 j 
 
 90 
 
 7 
 
 j 
 
 1 
 
 3 
 
 6] 
 
 
 4 
 
 6 
 
 
 10 
 
 0 
 
 6 
 
 31 
 
 10 
 
 J 
 
 2 
 
 1 
 
 20 
 
 1 
 
 31 
 
 10 
 
 1 
 
 
 
 
 6 
 
 
 
 4 
 
 
 
 18 
 
 
 
 267 
 
122 
 
 THE NORTHERN BITUMINOUS COAL FIELD, 
 
 [bull. 65. 
 
 Section near Gresson , Pennsylvania . — An oil boring near Cresson, on 
 the summit of the Alleghany Mountains, gives the following measure- 
 ments (Fig. 84) for the Lower Coal Measures (H 2 page 
 30 ): 
 
 Boring at Cresson , Cambria County , Pennsylvania. 
 
 [See map,H r.] 
 
 
 Ft. in. 
 
 1. Coal, Upper Freeport 5 
 
 2. Limestone, Upper Freeport 2 
 
 3. Mixed drilling 39 
 
 4. Coal, Lower Freeport 4 
 
 5. Shelly “soapstone” (sandstones and shales) 115 
 
 6. Cannel coal * 0 10 
 
 7. Slate 35 
 
 8. Coal, mixed with sandstone w 49 
 
 9. Hard sandstone (No. XII). 
 
 Total 249 10 
 
 Section at Bennington , Pennsylvania. — Just over the 
 crest of the Alleghany Mountains, at Bennington, Blair 
 ^ea^c'resson^a 11 County, the following section (Fig. 85) of this series has 
 been carefully worked out by Mr. John Fulton and 
 Franklin Platt (H 2 , pp. 3, 4) : 
 
 hT 
 
 isT 
 
 Bennington , Blair County , Pennsylvania. 
 
 [See map, Hr.] 
 
 Ft. in. 
 
 Coal, Upper Freeport 
 
 Fire clay, impure 2 ) 
 
 Sandstones and black slates 20 I 
 
 Limestone, Upper Freeport 3 ^ 
 
 Ferruginous slates ami shales 20 
 
 Sandstones and sandy shales. 20 j 
 
 7. Coal 
 
 Fire clay 1 1 
 
 Sandstone, drab 21 } 
 
 10. Black slates 20 
 
 11 . 
 
 12 . 
 
 13 
 
 14 , 
 
 15, 
 
 16, Slates 12 6 j 
 
 Coal, Upper Kittanning. 
 
 Drab slates, with iron balls 11 
 
 Sandstone 0 
 
 Blue slates 13 
 
 Sandstone, massive 15 
 
 '. Coal, 
 
 
 ( Coal 
 
 ...O' 
 
 6" ) 
 
 Middle Kittann>ng. . . 
 
 . < Slate — 
 
 ... 0 ' 
 
 6" > 
 
 
 ( Coal 
 
 ... V 
 
 
 Fire clay, impure 6 
 
 Sands one 12 
 
 Slate 1 
 
 Coal 0 
 
 Sandstone 7 
 
 Black slates 8 
 
 Coal, Lower Kittanning 
 
 Shales .• 
 
 Black slates 
 
 Coal, Clarion 
 
 Slates 
 
 Gray sandstone ... 
 
 Coal, Brookville. 
 
 Fire clay 
 
 Sandstone, massive, No. XII. 
 
 Total 
 
 Ft. in. 
 5 6 
 
 65 
 
 3 
 
 42 
 
 2 10 
 52 1 
 
 2 8 
 
 35 
 
 3 
 
 
 29 
 
 V 34 
 
 2 
 
 1 
 
 23 
 
 4 
 
 } 27 
 
 
 4 
 
 
 5 
 
 Fig. 85.— Section at 
 Bennington, Pa. 
 
 283 8 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 123 
 
 Section at Clearfield , Pennsylvania . — At the town of Clearfield, Clear- 
 field County, Pennsylvania, the following section (Fig. 86) was made 
 
 by the writer : 
 
 Clearfield, Pennsylvania . 
 
 [See map, E s.] 
 
 ( Coal, bony. V 3"] 
 
 I. Coal, Upper Freeport ...<j gjjj; f_°°^ J', y> > 
 
 I Coal. "I"” r 6" j 
 
 2. Concealed, and shales 
 
 3. Coal, Lower Freeport 
 
 4. Shales 
 
 5. Sandstone, massive, gray, Freeport 
 
 6. Shales, sandy *1 
 
 7. Coal, Middle Kittanning 
 
 8. Shales, and concealed 
 
 9. Coal, Lower Kittanning 
 
 10. Sandy shales 
 
 II. Fir e clay 
 
 1 2. Sandstone, flaggy - 
 
 13. Shales, dark 
 
 ( Coal, slaty V 6" I 
 
 14. Coal, Clarion < Fire clay'and shales. 8' 0" > 
 
 ( Coal, good 1- 0" ) 
 
 15. Fire clay and shales 
 
 ( Coal, slaty. O' 4") 
 
 16. Coal, Brookville — < Shale O' 12" > 
 
 (Coal O' 8" ) 
 
 17. Fire clay and concealed 
 
 18. Hard massive sandstone, top of No. XII, in bed of Sus- 
 
 quehanna Elver. 
 
 Total i.. 
 
 Ft. Ft. in. 
 
 4 4 
 
 
 
 50 
 
 
 
 
 •2 
 
 6 
 
 10 
 
 
 
 
 35 
 
 [ 
 
 70 
 
 
 25 
 
 s 
 
 
 
 
 
 1 
 
 6 
 
 
 
 35 
 
 
 
 
 2 
 
 
 25 
 
 j 
 
 
 
 8 
 
 6 
 
 V 
 
 f 
 
 45 
 
 
 6 
 
 J 
 
 
 
 
 
 10 
 
 6 
 
 
 
 10 
 
 
 
 
 * 2 
 
 
 5 
 
 237 10 
 
 Section near Morrisdale , Pennsylvania . — "Near Morrisdale, Clearfield 
 County, the following section (Fig. 87) is reported by Mr. H. Marty n 
 Chance (H 7 , p. 61) : 
 
 Near Morrisdale, Clearfield County, Pennsylvania. 
 
 Fig. 87.— Section near 
 Morrisdale, Pa. 
 
 [See map, Ft.] 
 
 1. Coal, Upper Freeport - 
 
 2. Fire clay and shales 
 
 3. Coal, Lower Freeport 
 
 4. Fire clay 
 
 5. Limestone, Lower Freeport - 
 
 C. Slate and sandstone 
 
 7. Coal, Upper Kittanning 
 
 8. Fire clay 
 
 9. Limestone, Johnstown Cement 
 
 10. Fire clay and sandstone with iron ore 
 
 11. Black slate 
 
 12. Coal 
 
 13. Sandstone 
 
 C Coal 0' 6" i 
 
 14. Coal, Middle Kittanning. < Sandstone. 3' 3 " > 
 
 (Coal 0' 10" ) 
 
 15. Sandstone 
 
 16. Slate 
 
 17. Coal, Lower Kittanning 
 
 18. Interval to top of No. XII, estimated, about 
 
 Total 
 
 Ft. in. 
 
 8 10 
 8 9 
 
 0 9 
 
 15 6 
 
 25 8 i 
 
 3 4 l 
 
 Ft. in. 
 2 6 
 32 6 
 
 4 6 
 
 43 6 
 
 2 10 
 
 39 6 
 
 4 7 
 29 
 
 5 6 
 75 
 
 239 5 
 
124 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section at Sterling Mines, near Houtzdale, Pennsylvania . — At the 
 Sterling mines of R. H. Powell’s Sons & Co., Clearfield County, a 
 diamond-drill boring was sunk through the Lower Coal Measures, be- 
 ginning 10 feet below the level of the main coal mined in that region. 
 I copied the record of this bore hole from the office of the company, 
 and it, combined with the surface exposures, gives the following suc- 
 cession (Fig. 88) : 
 
 Boring at Sterling Mines , near Houtzdale, Clearfield County, Pennsylvania . 
 
 1. Coal, Upper Freeport.. . 
 
 2. Concealed 
 
 3. Surface material in drill 
 
 4. Dark slate 
 
 [See map, G s.] 
 
 f Done coal 0' 10" ? 
 
 I Coal, sometimes a thin slate in center.. 4' 6" 5 
 
 liole. 
 
 5. Coal, Lower Freeport. .. 
 
 6 . 
 
 2 ‘ 7. 
 
 f Black shale and coal 1' 6" 1 
 
 I Shale, sandstone, and slate 8' 6" 
 
 Soft shale 1' 0" } 
 
 I Sandstone V 0" j 
 
 ( Coal 1' 0" J 
 
 50' 
 
 Fig. 88. — Section at 
 Sterling Mines, 
 near Houtzdale, Pa. 
 
 Sandy shale 
 
 Hard sandstone, Freeport 
 
 Dark slate 
 
 Coal, Upper Kittanning . . . 
 
 Fire clay 
 
 Dark slate 
 
 Coal, Middle Kittanning . . 
 Slate 
 
 Sandy shale 
 
 Slate 
 
 Coal, Lower Kittanning 
 
 Fire clay 
 
 Slate 
 
 Sandstone, close, hard . 
 
 Shales 
 
 Coal, Clarion 
 
 Hard slate 
 
 Ft 
 
 10 1 
 
 16 \ 
 16 J 
 
 7 J 
 
 n 
 
 9 
 
 32 
 
 21 
 
 Ft. in. 
 5 4 
 
 42 
 
 13 
 
 50 
 
 33 
 
 Total. 
 
 63 
 
 241 4 
 
 The coal at the top of this hist section has been identified as the 
 Lower Freeport bed, throughout the Clearfield region, by Messrs. Platt, 
 Chance, and other Pennsylvania geologists ; but it seems to me that 
 this section, taken in connection with the one at Clearfield (Fig. 86), 
 tends to prove that the coal in question is the Upper Freeport. This 
 interpretation is further confirmed by the presence of the Lower Ma- 
 honing sandstone on above No. 1, and a thin coal, the Mahoning bed, 
 at 60 to 80 feet above the latter, while crowning the hills is the Upper 
 Mahoning sandstone, whose top is 100 feet above No. 1. Then, too, the 
 structure of the coal itself is the same as the Upper Freeport, a few 
 miles distant, where it is mined along the Pennsylvania Railroad, in 
 the edge of Blair County. , 
 
WHITE. 1 
 
 THE LOWER COAL MEASURES. 
 
 125 
 
 Section at Shoup’s Run , Broad Top Basin , Huntingdon County , Penn- 
 sylvania. — In the Broad Top coal basin, Shoup’s Bun, Huntingdon 
 County, Pennsylvania, the Lower Coal Measures exhibit 
 the following structure (Fig. 89), as given by the writer 
 in T 3 , Geological Survey of Pennsylvania, page 46 : 
 
 100 ’ 
 
 so 
 
 Shoup’s Bun, Broad Top Basin, Huntingdon County , Pennsylvania. 
 
 [See map, J t.] 
 
 1. Coal, Upper Freeport 
 
 2. Sandy shales and sandstone . 
 
 3. Coal, Upper Kittanning 
 
 4. Shales and sandstone 
 
 5. Coal, Middle Kittanning 
 
 6. Shales and shaly sandstone. . 
 
 7. Coal, Lower Kittanning 
 
 Fig. 89. — Section 8 - Shales and concealed. .. 
 
 at Shoup’s Run, Massive conglomerate. 
 Broad lop Ba- 
 sin, Huntingdon 
 
 County, Pa. Total 
 
 Ft. 
 
 1 
 
 100 
 
 2 
 
 16 
 
 4 
 
 50 
 
 6 
 
 20 
 
 199 
 
 Section in East Broad Top Basin , Huntingdon County , Pennsylvania . — 
 In the East Broad Top region of Huntingdon County the structure is 
 thus (Fig. 90) given by Mr. H. N. Sims (T 3 , p. 68) : 
 
 East Broad Top Basin, Huntingdon County , Pennsylvania. 
 
 [See map, J t.] 
 
 1. Coal and slate, Upper Freeport 
 
 2. Concealed 
 
 •3. Conglomerate, small pehhles 
 
 4. Massive, light gray, pebbly sandstone, slightly argilla- 
 
 ceous at top 
 
 5. Concealed 
 
 6. Sandstone, micaceous 
 
 7. Concealed to top of shaft 
 
 8. Dark gray slate with iron ore balls 
 
 9. Sandstone, micaceous, dark gray 
 
 C Coal 2' 7" 
 
 10. Coal, Upper Kittanning < Black slate 
 
 ( Coal 
 
 11. Sandstone, slaty 
 
 12. Coal, MiddlO Kittanning 
 
 13. Concealed 
 
 14. Blue clay shales 
 
 15. Concealed : 
 
 16. Yellow shaly sandstone 
 
 17. Dark gray sandy slate 
 
 18. Black slate, sandy 
 
 Ft. in. 
 2 
 
 Ft. in. 
 
 10 
 
 10 
 
 69 
 
 4 6 > 165 4 
 
 2 i 
 
 34 10 ! 
 
 2' 7") 
 
 O' 
 
 O' 2"S 
 
 Fig. 90. — Section in Fast 
 Broad Top Basin, Hunt- 
 ingdon County, Pa. 
 
 C Coal, top bench 1' 6" 
 
 19. Coal, Lower Kittanning < II ml slate, parting. 0' 4" 
 ( Coal, bottom bench. 2' 0" 
 
 Total 
 
 3 3 
 2 9 
 
 35 
 
 3 10 
 216 2 
 
126 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 (BULL. 65. 
 
 Section in Broad Top Basin . Bedford County , Pennsylvania.— In tlie 
 Broad Top Basin of Bedford County, Pennsylvania, the structure is 
 thus (Fig. 91) given by Stevenson (T 3 , pp. 59 and 60): 
 
 Broad Top Basin, Bedford County, Pennsylvania. 
 
 [See map, J t.] 
 
 1. Coal, Upper Freeport 
 
 2. Shales and sandstones 
 
 3. Coal, Upper Kittanning 
 
 4. Clay 
 
 5. Sandstone 
 
 6. Coal, Middle Kittanning 
 
 7. Clay 
 
 8. Sandstone and shale 
 
 9. Coal, Lower Kittanning 
 
 10. Clay 
 
 11. No. XII, conglomerate. 
 
 Total 
 
 Ft. 
 
 50 
 
 Ft. in. 
 5 
 93 
 
 1 6 
 2 
 28 
 4 
 
 56 
 
 195- 
 
 & lection act Piedmont , West Virginia . — In the vicinity of Western port, 
 Maryland, where the North Potomac cuts across the Cumberland or 
 George’s Creek coal basin, the Lower Coal Measures exhibit the follow- 
 ing succession (Fig. 92) : 
 
 Piedmont , Mineral County , West Virginia. 
 
 !' V 
 
 (lllllllllllllllIHll 
 
 Y 
 
 zd 
 
 1. Coal, Upper Freeport. 
 
 Fig. 92. — Section at 
 Piedmont, W. Va. 
 
 [See map, N p.] 
 
 Coal 2' 
 
 Shale and hone. 1 
 Coal 2 
 
 Concealed 
 
 Shale, bluish 
 
 Coal, Lower Freeport 
 
 Fire clay 
 
 Concealed 
 
 Sandstone, hard 
 
 Sandstone, shaly 
 
 Shales, sandstone, and concealed 
 
 :i 
 
 Coal, Upper Kittanning.. J £j^ mill0US slate 
 
 2 '} 
 
 Ft. 
 
 10 ] 
 
 10 3 
 
 2 1 
 10 | 
 2 
 5 
 
 55 
 
 10 1 
 50 [> 
 
 5 J 
 
 Dark shales, and concealed 
 
 Massive sandstone, gray 
 
 Shales, drab 
 
 f Coal, slaty . . 1' 0" ] 
 
 Coal, bon v . o' 8" ‘ 
 
 Coal, Lower Kitlanning <{ Coal, good . . 1' 4" J- 
 
 | Slate, hard . ()' h" | 
 
 [Coal, good.. 2 6 "J 
 
 Fire clay, sandy 
 
 Shales, with nodular iron ore 
 
 Fire clay, impure 
 
 Flaggy sandstone , 
 
 Concealed 
 
 Fire clay, sandy 
 
 Flaggy sandstone and sandy shales 25 J 
 
 Concealed, and sandy shales a 
 
 Top of No. XII. 
 
 3 1 
 
 2 
 
 4 
 
 20 > 
 25 
 10 
 
 Ft. in. 
 5 
 
 65 
 
 6.J 
 
 8Q 
 
 40 
 
 307 6i 
 
 Total 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 127 
 
 Section near Maple Swamp water tank, West Virginia Central Rail- 
 road, Mineral County, West Virginia . — Near Maple Swamp water tank, 
 on the West Virginia Central Railroad, Mineral County, 
 West Virginia, these beds exhibit the following structure 
 (Fig. 93) : 
 
 On North Potomac at Maple Swamp water tank, West Virginia Central 
 
 Railroad. 
 
 [See map, N p.] 
 
 Ft. in. 
 
 C Coal O' 5") 
 
 1. Coal, Upper Freeport . . < Bone and slate . . 1' 4" > 4 3 
 
 (Coal 2' 6" } 
 
 2. Concealed - 60 
 
 3. Coal, Lower Freeport 1 2 
 
 4. Concealed 55 
 
 Coal, Upper Kittanning 
 Concealed, and slate 
 
 6 
 
 35 ' 
 
 C Coal 3' 0") 
 
 Coal, Lower Kittanning < Slate 2' 0" > 
 
 ^ (Coal V 5") 
 
 Concealed, and sandstone 85 
 
 Coal, Clarion 2 6 
 
 Shales, and concealed 45 
 
 Massive sandstone, top of No. XII. 
 
 Total 305 4 
 
 Section near Thomas, West Virginia. — At the head of 
 the North Potomac and on the Cheat River side of the 
 great Alleghany watershed, we get a fine exposure of the 
 Lower Coal Measures in the vicinity of Thomas, Tucker 
 County, West Virginia. The exposures have been made 
 by the mining and grading operations of the West Vir- 
 ginia Central Railroad, and there the section reads as follows (Fig. 94): 
 
 Fm.93.-On North 
 Potomac at Ma- 
 ple Swamp Wa- 
 ter Tank, West 
 Virginia Cen- 
 tral .Railroad. 
 
 Near Thomas, Tucker County , West Virginia. 
 
 [See map, O o.] 
 
 1. Coal, Upper Freeport 
 
 Coal 
 
 Bone and bony co; 
 Coal 
 
 2. Sandy shales, weathering reddish 
 
 C Coal 
 
 3. Coal, Lower Freeport . . < Shale 
 
 ( Coal 
 
 4. Concealed 
 
 5. Massive pebbly sandstone, Freeport 
 
 6. Coal, streak, Upper Kittanning 
 
 7. Fire clay and shales 
 
 f Coal, good 1' 
 
 Slate O' 
 
 
 8. Coal, Middle and Lower 
 Kittanning 
 
 Fig. 94. — N ear 
 Thomas, Tucker 
 County, W.Va. 
 
 9. Concealed 
 
 10. Massive sandstone 
 
 11. Shales 
 
 12. Iron ore, bnhrstone 
 
 13. Limestone, ferriferous 
 
 14. Shales and sandstone 
 
 15. Coal, Clarion 
 
 16. Shales 
 
 IT Sandstone, top of No. XII. 
 
 Coal, good 1' 
 
 S.ate 0' 
 
 Coal, good 3' 
 
 Shale, gray 1' 
 
 Coal, slaty 3' 
 
 Ft. 
 
 Ft. in. 
 8 
 40 
 
 1 6 
 70 
 35 
 
 Total 
 
 273 6 
 
128 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section near Moatsville, Barbour County , West Virginia. — I^ear Moats- 
 ville, Barbour County, West Virginia, on the Tygart’s Valley River, 
 the following section of the Lower Coal Measures is ex- 
 posed (Fig. 95): 
 
 Near Moatsville , Barbour County, West Virginia. 
 
 sa' 
 
 
 Fig. 95. — Section 
 near Moats- 
 ville, W. Va. 
 
 [See map, O m.] 
 
 1. Coal, Upper Freeport 
 
 2. Concealed, and sandy shales ... 
 
 [ Slatv coal and slate O' G" 
 
 | Shale and lire clay.. 4' 0" 
 
 3. Coal, Lower Freeport.. <1 Coal .... 2' 0 
 
 Dark bony clay O' 3' 
 
 [Coal ' 1' 3" 
 
 4. Concealed 
 
 5. Sandstone, massive, gray 
 
 6. Concealed 
 
 7. Dark blue shale 
 
 8. Flaggy sandstone and concealed 
 
 9. Limestone, gray, Campbell’s Creek 
 
 10. Shales, and massive sandstone 
 
 f Coal 
 
 11. Coal, Lower Kittanning < Shales 
 
 ( Coal 
 
 12. Concealed 
 
 13. White pebbly sandstone, top of No. XII. 
 
 
 Ft. 
 
 Ft. in. 
 3 
 
 50 
 
 105 
 
 . 1 ' 6 " ) 
 i. 8' 0" V 
 . . 3' 0" > 
 
 Total 
 
 220 6 
 
 Section near Valley Falls , West Virginia. — In the vicinity of Valley 
 Falls, Taylor County, West Virginia, where the Chestnut Ridge anti- 
 cline brings the series above water level, the following succession is 
 visible (Fig. 96) : 
 
 Valley Falls , Taylor County, West Virg nia . 
 
 [See map, N 1.] 
 
 
 3 
 
 AO 
 
 
 W 
 
 
 
 11111 
 
 3 / 
 
 
 V? 
 
 w 
 
 iaf 
 
 
 
 i ) 
 
 
 ¥ 
 
 HUM! 
 
 
 
 5' 
 
 
 & 
 
 
 zo' 
 
 : m & 
 
 isf 
 
 
 l c 
 
 a' 
 
 Coal, Upper Freeport 
 Concealed and shales 
 
 Sandstone 
 
 Blue shales 
 
 «a‘ 5. Coal, Lower Freeport. 
 
 Dark shales 
 
 Sandstone, Freeport 
 Shales, blue 
 
 f Coal O' 3" 
 
 I Slate, gray 0' 6" 
 
 I Coal ‘ 1' 3'' 
 
 Shale 2' 11" 
 
 I Coal, bony cannel. 0' 6" 
 
 I Shale, gray 0' 8" 
 
 [Coal..... . . 1' 3" 
 
 Ft. 
 
 40 
 
 15 
 
 4 
 
 Ft. in. 
 3 
 
 59 
 
 7 4 
 
 9. Coal, Upper Kittanning 
 
 10 . 
 11 . 
 12 . 
 
 13. 
 
 14. 
 
 15. 
 
 16. 
 
 17. 
 
 18. 
 
 19. 
 
 20 . 
 
 r 45 2i. 
 
 22 . 
 
 23. 
 
 Coal 
 Shale, gray 
 Coal, bony 
 
 . . . . 3' 1" ) 
 ay. 0' 1" > 
 y.. 0' 7" ) 
 
 ?) 
 
 24. 
 
 —Section 25 - 
 
 Fig. 
 
 near Valley Falls, 
 W. Va. 
 
 Shales, dark grayish 
 
 Coal, Middle Kittanning 
 
 Shales and flaggy sandstone 
 
 Limestone, siliceous a . 
 
 Sandstone, flaggy 2 ( 
 
 Shales, containing iron ore nodules 5 
 
 Limestone, dark blue, Campbell’s Creek 1 
 
 Shales 20 
 
 Coal, Lower Kittanning 
 
 Fire clay 5 
 
 Sandstone, flaggy o 
 
 Sandy shales, and concealed 20 
 
 Sandstone, hard, micaceous 15 
 
 C Coal.. O' 2" 
 
 Coal, Clarion < Shale. 0' 10 
 
 (Coal.. 0' 2" 
 
 Shales, and concealed 
 
 Sandstone, massive, top of No. XII. 
 
 2 ") 
 
 55 
 
 Total 
 
 258 3 
 
 In this last sectiou, and also in the preceding one (Fig. 95), a bed of 
 impure, siliceous limestone occurs in the shale interval above the Lower 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 129 
 
 Kittanning coal. It occup : es the same geological horizon as the thin, 
 siliceous limestone above, the Campbell’s Creek (Lower Kittanning) 
 coal on the Big Kanawha River, and hence I have identified it with 
 that stratum. 
 
 Section near Nuzum’s Mill , Marion County , West Virginia. — Farther 
 down the stream (Tygart’s Valley River) the following structure (Fig. 
 97) was observed on the right bank, below Nuzum’s Mill, Marion 
 County, West Virginia: 
 
 Fig. 97.— Section near 
 Nuzum’s Mill, Marion 
 County, W. Va. 
 
 1 . 
 
 2 . 
 
 3. 
 
 7. 
 
 10 . 
 
 13. 
 
 17. 
 
 21 . 
 
 23. 
 
 25. 
 
 26. 
 
 27. 
 
 28. 
 
 Near Nuzum’s Mill , Marion County, West Virginia. 
 
 [See map, N 1.] 
 
 Coal, Upper Freeport 
 
 Clay 
 
 Sandstone 
 
 Limestone, Upper Freeport 
 
 Shales and concealed 
 
 Sandstone, coarse 
 
 Shales, sandy, drab 
 
 Coal, Lower Freeport 
 
 Shales and concealed 
 
 Massive sandstone, Freeport 
 
 Coal, Upper Kittanning 
 
 Shales, dark, sandy, with limy beds 
 
 Black slate — 
 
 Coal, slaty, Middle Kittanning 
 
 Shales and sandy beds 
 
 Coal. Lower Kittanning 
 
 Fire clay 
 
 Sandstone, flaggy 
 
 Dark shales with iron ore nodules 
 
 Iron ore, Ferriferous limestone horizon 
 
 Dark shales 
 
 Black slate 
 
 Coal, Clarion 
 
 Fire clay, sandy 
 
 Dark shales, with iron ore nuggets near middle 
 
 Flaggy sandstone 
 
 Concealed and coal blossom, Brookville 
 
 No. XII, conglomerate. 
 
 Total - 
 
 Ft. in. 
 
 2 
 
 15 
 
 3 
 
 13 
 
 10 
 
 15 
 
 30 
 
 25 
 
 1 
 
 I 
 
 t 
 
 J 
 
 40 
 
 3 
 
 5 
 
 5 
 
 12 
 
 0 
 
 5 
 
 2 
 
 1 
 
 1 
 
 i 
 
 Ft. in. 
 
 3 
 
 58 
 
 5 7 
 
 55 
 
 2 
 
 43 
 
 1 
 
 20 
 
 5 
 
 30 
 
 0 1 
 
 33 
 
 6 
 
 .. 261 8 
 
 Fig. 98.— Sect i on 
 under Clarksburg, 
 W. Va. 
 
 Section under Clarksburg, West Virginia. — From the 
 records of the Despard gas well boring, at Clarksburg, 
 Harrison County, West Virginia, as furnished by T. M. 
 Jackson, civil engineer, we get the structure of the 
 Lower Coal Measures there, as follows (Fig. 98): 
 
 Under Clarksburg, West Virginia. 
 
 [See map, O k.] 
 
 1. Upper Freeport coal 
 
 2. Shales# sandy 
 
 3. Sandstone, white 
 
 4. Shales 
 
 5. Sandstone, white, Freeport 
 
 6. Sandstone, dark . 
 
 7. Coal, Middle Kittanning 
 
 8. Shale, black 
 
 9. Sandstone, gray 
 
 10. Sandstone, white 
 
 11. Coal, with slate. Lower Kittanning 
 
 12. Sandstone, hard, gray 
 
 13. Sandstone, bard, white 
 
 14. Shale 
 
 15. Top of No. XII, white sandstone. 
 
 Total 
 
 Ft. 
 
 Ft. 
 
 absent 
 
 291 
 
 
 7 
 
 
 79 
 
 124 
 
 il | 
 
 io i 
 
 Si 
 
 1 
 
 49 
 
 16 ^ 
 
 4 
 
 4) 
 
 36 t 
 14 5 
 
 54 
 
 232 
 
 The Lower Kittanning bed is here more than 1,000 feet betew the 
 summits of the hills. 
 
 Bull. 65 9 
 
130 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section under Parkersburg , West Virginia. — At Parkersburg, Wood 
 County, West Virginia, the following structure (Fig. 99) is given by the 
 record of the Camden Consolidated Oil Company’s drill 
 hole, on the authority of K. A. Cole, superintendent: 
 
 Under Parkersburg, West Virginia » 
 
 [See map, N f.] Ft. 
 
 1. Upper Freeport coal - absent 
 
 2. Shales, gray and black 170 
 
 3. Coal, Lower Kittanning 7 
 
 4. Shales, gray - 98 
 
 5. Top of No. XII. 
 
 Total 
 
 275 
 
 Fig. 99. — Section 
 under Parkers- 
 burg, W.Va. 
 
 The Lower Kittanning bed is the only one in the series 
 here, but it has a good thickness, though lying 1,100 feet 
 below the bed of the Ohio Kiver, and 1,500 feet under 
 the surface of the hill summits. 
 
 Section under Wheeling , West Virginia . — 
 
 Under Wheeling, West Virginia, where the 
 top of the series is more than 400 feet below 
 water level, the record of the Central Glass 
 Company’s drill hole for gas gives the fol- 
 lowing structure (Fig. 100) : 
 
 Under Wheeling, West Virginia. 
 
 [See map, Kj.] Ft. 
 
 g coal and 450 feet under 
 
 7 
 
 1. Coal, Upper Freeport— 556 feet under Pittsburg coal and 450 feet under 
 
 Ohio Kiver level 
 
 2. Sandstone and shales 96 
 
 3. Coal, Upper Kittanning 5 
 
 4. Shales and sandstone 112 
 
 5. Top of No. XII. 
 
 Total 220 
 
 
 rrrrrvv?! 
 
 50 
 
 Section at mouth of Little Beaver , on the 
 Pennsylvania- Ohio State line. — At the ^nd^Vheeto^ 
 mouth of Little Beaver, on the Pennsyl- W - Va - 
 vania-Ohio State line, and the northern point of the 
 West Virginia “Pan-Handle,” the structure is as fol- 
 lows (Fig. 101): 
 
 1.05’ 
 
 Ohio and Pennsylvania line, v^outh of Little Beaver. 
 
 60 ' 
 
 Fig. 101. — Section at 
 mouth of Little 
 Heaver. 
 
 [See map, G j.] 
 
 1. Coal, Upper Freeport 
 
 2. Sandy shales 
 
 3. Coal, Lower Freeport 
 
 4. Sandy shales 
 
 5. Sandstone, massive 
 
 6. Sandy shales .. 
 
 7. Coal, Middle Kittanning 
 
 8. Fireclay - 
 
 9. Shales, containing nodules of iron ore ..... 
 
 10. Coal, Lower Kittanning 
 
 11. Fire clay 
 
 12. Sandy shales and shaly sandstone 
 
 13. Limestone, Ferriferous 
 
 14. Sandy shales 
 
 15. Bituminous shale, Clarion coal 
 
 16. Shales, sandy 
 
 17. Massive sandstone, top of No. XII. 
 
 Ft. 
 
 Ft. in. 
 50 
 
 16 
 
 Total. 
 
 273 6 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 131 
 
 Section near Sprucevale , Cotunxbiana County , Ohio . — Northward up 
 the Little Beaver the column of rocks is very much the same as at the 
 OhioBiver, as may be seen from the following section (Fig. 102) taken 
 near Sprucevale, Columbiana County, Ohio : 
 
 
 Fig. 102.— Section 
 near Sprucevale, 
 Columbiana 
 County, Ohio. 
 
 Near Sjprucevale, Columbiana County, Ohio. 
 
 [See map, G j.] 
 
 1. Coal, Upper Freeport 
 
 2. Fireclay 
 
 3. Limestone, Upper Freeport 
 
 4. Shales, and concealed 
 
 5. Coal, Lower Freeport 
 
 6. Concealed 
 
 7. Sandstone, massive, Freeport 
 
 8. Coal, Middle Kittanning 
 
 9. Concealed 
 
 10. Coal, Lower Kittanning 
 
 11. Fire clay and shales 
 
 12. Limestone, siliceous, Upper Ferriferous 
 
 13. Shales, gray 
 
 14. Shales, dark 
 
 , _ T . . C Lower Ferriferous . . ? 
 
 15. Limestone } Putnam Hill \ — 
 
 16. Coaly .shales, Clarion . 
 
 17. Fire clay 
 
 18. Concealed, to top of No. Xll 
 
 Total 
 
 Ft. Ft. 
 
 thin 
 
 25 
 
 2 
 
 5 
 
 1 
 
 5 
 
 5 
 
 291 
 
 Here we get the beginning of an important feature in Ohio Lower 
 Coal Measure stratigraphy, viz : a duplication of the Ferriferous lime- 
 stone. The lower bed, No. 15, occupies the regular horizon of the 
 Pennsylvania u Ferriferous ” bed, but there comes in above it here a 
 stratum, No. 12, of siliceous limestone, not seen anywhere in Pennsyl- 
 vania, but becoming the ore-bearing limestone of the Ohio series, and 
 known as the “ Gray ” limestone, the ore on its top being of the same 
 character as the Buhrstone ore of Pennsylvania and apparently identi- 
 cal with it. 
 
 Prof. Orton, director of the Ohio Geological Survey, thinks that on 
 entering Ohio the Great Ferriferous limestone of Pennsylvania splits 
 into two portions, the upper part representing the “ Gray ” limestone 
 and the lower or blue portion of the Ferriferous representing the 
 “ Putnam Hill” bed of Ohio. This seems to be the most probable view 
 of the matter, though it is barely possible that the lower or Putnam 
 Hill stratum is an entirely new deposit, and has no representative in 
 Pennsylvania, or this may b« true with reference to the upper limestone, 
 No* 12* 
 
132 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section between New Lisbon and Leetonia , Ohio . — In going northwest- 
 ward from Sprucevale, a very rapid change takes place in the lower 
 portion of the column, since it rapidly contracts, as will be seen from 
 the following section (Fig. 103), made in the vicinity of the cement 
 works, between New Lisbon and Leetonia, Ohio : 
 
 and Leetonia, Ohio. 
 
 Between New Lisbon and Leetonia, Ohio. 
 
 [See map, G i.] Ft. Ft. in. 
 
 Coal, Upper Freeport (not seen) 
 
 Concealed 30 ^ 
 
 Sandstone 10 > 50 
 
 Shales, chocolate 10 ' 
 
 Coal, Lower Freeport 0 2 
 
 Fireclay 4 
 
 Limestone, Lower Freeport 4 
 
 Concealed, and sandstone 50 
 
 Shales 5 
 
 Coal, Lower Kittanning.. ^ i' — 6 6 
 
 Slate 1 1 
 
 Limestone and iron ore, Upper Ferriferous 1 ! 
 
 Concealed, and shales 35 { 39 
 
 Limestone, fossiliferoos.. { lgg3a*»» } - 2 1 
 
 Coal, Clarion 3 
 
 Fire clay 10 > 
 
 Interval to top of No. XII 25 3 ^ 
 
 Total 196 8 
 
 Section near Zanesville , Ohio . — In the vicinity of Zanesville, Muskin- 
 gum County, Ohio, the section of the Lower Coal Measures reads as 
 follows (Fig. 104), at the type locality of the Putnam Hill limestone 
 (Vol. Y, Ohio Geology, p. 96) : 
 
 Zanesville, Muskingum County, Ohio. 
 
 Fig. 104. — Section 
 n ear Zan es ville, 
 Ohio. 
 
 [See map, K e.] 
 
 1. Coal, Upper Freeport 
 
 2. Fire clay 
 
 3. Limestone, Upper Freeport 
 
 4. Concealed 
 
 5. Coal, Lower Freeport 
 
 6 . Fire clay 
 
 7. Concealed 
 
 8 . Sandstone, Freeport 
 
 9. Coal, Middle Kittanning 
 
 10. Fire clay 
 
 11. Shales, with ore nodules 
 
 12. Coal, Lower Kittanning 
 
 13. Fire clay 
 
 14. Limestone, Upper Ferriferous 
 
 15. Sandstone .. 
 
 16. Shales 
 
 17. Limestone... 
 
 Lower Ferriferous ? 
 
 Putnam Hill 3 
 
 18. Shales, dark 
 
 19. Coal 
 
 20. Fire clay and dark shales 
 
 21. Coal, Clarion.. * 
 
 22. Fire clay, shales, and concealed, to base of Lower Coal 
 
 Measures 
 
 Ft. 
 
 Ft. in. 
 
 
 4 
 
 2 l 
 
 
 1 ( 
 
 42 
 
 39 ’ 
 
 1 
 
 6 ) 
 
 
 34 [ 
 
 60 
 
 20 J 
 
 4 
 
 6 \ 
 18 3 
 
 24 
 
 
 4 
 
 4 1 
 
 
 2 [ 
 44 
 
 56 
 
 thin 
 
 15 
 
 Total. 
 
 225 0 
 
THE LOWER COAL MEASURES. 
 
 133 
 
 Section near Shawnee and McCuneville , Ohio . — In the vicinity of 
 Shawnee and McCuneville, Perry County, Ohio, these beds exhibit the 
 following structure (Fig. 105) : 
 
 Vicinity of Shawnee and McCuneville, Perry County, Ohio. 
 
 [See map, M d.] 
 
 Ft. in 
 
 1. Coal, Upper Freeport (not seen) 
 
 2. Fire clay and shales containing “ Buchtel ” ore. 15 
 
 3. Limestone, Upper Freeport 2 ( 
 
 4. Shales, and concealed 25 
 
 5. Coal, Lower Freeport 1 ( 
 
 Clay, with iron ore 10 
 
 7. Concealed, and shales 25 
 
 2 ' 0 " 
 
 coal 
 
 Coal 
 
 8. Coal, Middle Kittanning ■( dark gray 
 
 Fig. 105.— Vicinity 
 of Shawnee and 
 McC u n e v i 1 1 e, 
 Perry County, 
 Ohio. 
 
 16. Fire clay 10 
 
 17. Massive sandstone, top of No. XII. 
 
 10 8 
 
 Coal. 
 
 Slate O' 
 
 Coal 3' 
 
 Clay, with calcareous ore 10 
 
 10. Concealed, and shales 20 
 
 11. Coal, Lower Kittanning 
 
 12. Clay 5 
 
 13. Ferriferous ore and flint 1 
 
 14. Sandy shales 40 
 
 is ( Lower Ferriferous ? . 
 
 15. Limestone $ Putnam Hill j 1 
 
 Total 176 8 
 
 Section near Buchtel , Ohio . — In the vicinity of Buchtel, at the line of 
 Hocking and Athens Counties, the Lower Coal Measures exhibit this 
 structure (Fig. 106) : 
 
 Hocking Valley, near Buchtel, Athens County, Ohio. 
 
 [See map, N c.] Ft. Ft. in. 
 
 Fig. 106.— Hock- 
 ing Valley, near 
 Buchtel, Athens 
 County, Ohio. 
 
 ( Coal, slaty 1' 3"' 
 
 j Shale 0' 3" 
 
 I Coal 1' 3" 
 
 1. Coal, Upper Freeport.. <( Shale 0' 3" 
 
 I Coal. 1' 3" 
 
 Shale 0' 3" 
 
 [Coal 1' 3", 
 
 2. Fire clay and shale . . 
 
 3. Limestone, Freeport 
 
 4. Concealed, and shales 
 
 C Coal V 6 "'k 
 
 5. Coal, Lower Freeport . . < Slate O' 1" > 
 
 (Coal V 6"} 
 
 6. Concealed 
 
 (Bone coal O' 6"1 
 
 Coal 2' 0"l 
 
 7. Coal, Middle Kittanning < ® ’!!!!*!’!! v %'( 
 
 ( Slate."!!.’!”.’.*.’ 0' 1" 
 
 l Coal 1' 6" J 
 
 8. Concealed 
 
 9. Coal, Lower Kittanning 
 10. Concealed 
 
 11. Iron ore 
 
 12. Limestone, Ferriferous ... 
 
 13. Interval to top of No. XII 
 
 Total , 
 
 5 9 
 
 5) 
 
 5 j> 50 
 40 j 
 
 3 1 
 
 30 
 
 6 1 
 
 30 
 
 1 
 
 10 
 
 1 
 
 2 
 
 40 
 
 178 11 
 
134 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65. 
 
 Section on Meeker's Run , near N’elsonville , Ohio. — On Meeker’s Run, 
 near Nelsonville, Athens Couuty, Ohio, the structure of the Lower 
 Coal Measures is thus (Fig. 107) given by Prof. Orton in Yol. Ill, Ohio 
 Geology, page 926 : 
 
 On Meelcer's Bun , near Nelsonville, Athens County, Ohio. 
 
 [See map, N c.] 
 
 1. Coal, Tipper Freeport. 
 
 2. Fire clay 
 
 3. Shales 
 
 4. Buchtelore 
 
 5. Shales 
 
 6. Straitsville ore 
 
 Fig 107.— Section 
 on Meeker’s Run, 
 Athens County, 
 Ohio. 
 
 7. Shawnee or Buff limestone (Upper Freeport) 
 
 8. Sandstone 
 
 9. Coal, Lower Freeport 
 
 10. Shales. 
 
 11. Limestone, Lower Freeport . . { } 
 
 12. Sandstone 
 
 13. Coal, Upper Kittanning .. 
 
 14. Fire clay 
 
 15. Sandstone 
 
 16. Shale 
 
 17. Coal 
 
 18. Fire clay 
 
 19. Shale 
 
 20. Snowfork ore 
 
 21. Sandstone 
 
 22. Coal, Lower Kittanning.. 
 
 23. Fire clay 
 
 24. Shales 
 
 25. Place for Baird ore 
 
 26. Place for Gray limestone 
 
 27. Interval to No. XII sandstone 
 
 Total 
 
 Middle Kittanning. 
 N elsonville seam . . . 
 
 Ft. in. 
 
 4 
 
 3 
 
 5 9 
 
 1 3 
 
 6 
 1 
 
 2 6 
 
 14 6 
 1 0 
 
 4 0 
 
 1 6 
 
 12 6 
 3 
 
 1 6 
 
 15 6 
 
 3 6 
 
 6 11 
 
 3 
 
 5 
 
 0 8 
 27 
 2 
 
 4 
 
 6 
 
 30 
 
 165 1 
 
 Section at Panther Hill, Scioto County , Ohio. — Farther to the southwest, 
 in Panther Hill, near Mt. Yernon Furnace, Scioto County, Ohio, these 
 rocks are given as follows (Fig. 108) in Yol. Y, Ohio Geology, p. 1038: 
 
 Panther Hill, Mt. Vernon Furnace, Scioto County , Ohio. 
 
 [See map, Q a.] 
 
 1. Coal, blossom, Upper Freeport 
 
 2. Shale, sandy 
 
 3. Concealed - 
 
 4. Sandstone, shaly 
 
 , 5. Coal, blossom, Lower Freeport 
 
 3a 6. Fire clay 
 
 7. Shale 
 
 8. Sandstone 
 
 9. Slate 
 
 as’ 10. Coal, Middle Kittanning 
 
 11. Shales, with iron ore (kidney) - 
 
 12. Sandstone, massive . 
 
 f Coal blossom 1 
 
 13. Coal, Lower Kittanning < Sandstone, shaly ... 7 > 
 
 45 (Coal blossom) 
 
 14. Concealed 
 
 15. Sandstone, white 
 
 16. Shale 
 
 17. Iron ore, “ Baird, ” buhrstone 
 
 3 18. Limestone, Ferriferous 
 
 19. Coal 
 
 20. Sandstone, white 
 
 21. Coal, Clarion 
 
 22. Shale 
 
 Fig. 10-.— Panther 23. Coal, Brookville 
 
 Hill, Mt. Vernon 24. Sandstone, top of No. XII. 
 
 Furnace, Scioto 
 County, Ohio. 
 
 Feet. 
 
 Feet. 
 
 HI 
 
 
 15 S 
 
 38 
 
 12 j 
 
 
 20 | 
 
 39 
 
 4 J 
 
 
 16 l 
 
 29) 
 
 45 
 
 
 7 
 
 8) 
 
 
 6 V 
 
 18 
 
 4) 
 
 
 blossom 
 
 16 
 
 blossom 
 
 Total. 
 
 175 
 
WniTE.] 
 
 THE LOWER COAL MEASURES. 
 
 135 
 
 Section near fronton, Oliio .-^ From the vicinity of Ironton, Ohio, Prof. 
 Orton reports the following' structure (Fig. 109) for the Lower Goal 
 Measures (Yol. Ill, Ohio Geology, p. 928): 
 
 Ironton, Lawrence County. Ohio. 
 
 [See map, R b.] 
 
 Ft. in. Ft in. 
 
 1. Coal, Upper Freeport 4 
 
 2. Fire clay . 2 1 
 
 3. Conglomerate and sandstone 29 
 
 4. Little yellow kidney or Monitor furnace ore 1 
 
 5. Concealed 2 l Qc 
 
 6. Buff limestone 2 ( 
 
 7. Shales 23 6 
 
 8. Yellow kidney ore (Moxahala) 1 | 
 
 9. Heavy sand rock . 37 6 J 
 
 10. Coal No. 6 (Sheridan coal), Middle Kittanning 3 
 
 11. Fireclay T 8 61 
 
 12. Black kidney ore 1 > 34 
 
 13. Sand rock 24 6 ) 
 
 14. Coal No. V (New Castle), Lower Kittanning 3 6 
 
 15. Fire clay 2 ) 
 
 16. Sand rock 23 6 V 31 6 
 
 17. Fireclay 6 ) 
 
 18. Limestone ore 1 
 
 19. Gray limestone, Ferriferous 5 
 
 20. Sand rock, Hearthstone quarries 60 6l 
 
 21. Conway coal No. 3, C. (Brookville) 2 > 64 6 
 
 22. Fireclay.. 2 ) 
 
 23. Top of No. XII, sandstone. 
 
 Total 244 6 
 
 40 ' 
 
 Fig. 110.— Section 
 in southern 
 Ohio, near Iron- 
 ton. 
 
 Section in southern Ohio , near fronton . — In the same 
 region of Ironton, but at a different locality, the writer 
 found the following structure (Fig. 110): 
 
 In southern Ohio, above Ironton. 
 
 [See map, S b.] 
 
 1. Coal, Upper Freeport 
 
 2. Shales and sandy beds 
 
 3. Coal, Lower Freeport 
 
 4. Massive sandstone 
 
 6. Shale 
 
 t Coal 1' l 
 
 | Fire clay 1' | 
 
 6. Coal, Middle Kittanning. %. ■[ Coal V )■ 
 
 Fire clay 2' | 
 
 [Coal 2 ' ) 
 
 7. Fire clay 
 
 8. Sandstone, massive 
 
 9. Coal, Lower Kittanning ; 
 
 10. Shales and fire clay 
 
 11. Limestone, Ferriferous 
 
 12. Firti clay and shales 
 
 13. Coal, Clarion 
 
 14. Shales, and concealed 
 
 15. Massive sandstone, top of No. XII. 
 
 Total 
 
 Ft. Ft. in. 
 
 2 
 
 50 
 
 3 
 
 7 
 
 5 * 
 
 40 3 
 
 45 
 
 2 6 
 
 25 
 
 5 
 
 10 
 
 1 
 
 40 
 
 235 6 
 
 This section differs but little from that found in western Pennsylva- 
 nia. The “Buhrstone” or “Baird” ore, which was not noted in this, 
 is present in other sections at its proper horizon on top of No. 11. The 
 Putnam Hill, or lower division of the Ferriferous limestone, seems to 
 have disappeared, either by coalescing with the upper one or failure of 
 deposition, and the same appears to be true of the Upper Kittanning 
 coal, unless it is to be found in the upper layers of the complex Middle 
 Kittanning No. G, which is not improbable. 
 
136 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section at Charleston , West Virginia . — As we leave the northwestern 
 margin of the Appalachian field in southern Ohio, and pass southeast- 
 ward toward the other or eastern side of the same, the 
 Lower Coal Measures thicken up quite rapidly, as will 
 be seen from the line of sections which will now be 
 given along the Great Kanawha River. The following 
 one (Fig. Ill), from the mouth of Elk River, at Charles- 
 ton, is the record of Edwards gas well No. 3. It begins 
 at the level of the Upper Freeport coal, and the record 
 was obtained from Mr. W. S. Edwards, the superintend- 
 ent of the gas company: 
 
 Under Charleston , Kanawha County , West Virginia, by bore hole near 
 mouth of Elk River. 
 
 [See map, S f.] 
 
 Ft. in. 
 
 1. Coal, Upper Freeport 3 
 
 2. Shales and slates 55 
 
 3. Coal, Lower Freeport 1 6 
 
 4. Sandstone and shales - 116 
 
 5. Coal, slaty, Upper Kittanning 5 
 
 6. Shales and sandstone 203 
 
 7. Sandstone, coarse, with gas and water 70 
 
 8. Coal, Clarion 
 
 9. Shales and sandstone 90 
 
 10. Shales 30 
 
 11. Top ofXo. XII, white sandstone. 
 
 Total 573 6 
 
 The thickness of the measures is here about three 
 times greater than in the Hocking Valley, 100 miles 
 north from Charleston. Just where this rapid thicken- 
 ing begins has not ^et been determined, owing to the 
 absence of reliable borings between the Hocking Valley 
 and Charleston, but it is probable that the most of it 
 comes in from the Ohio River southward to Charleston, 
 since the borings at Pomeroy and Hartford City disclose 
 no unusual thickness of the Lower Coal Measures. 
 
 The identification of coal No. 8 in the above section is 
 open to question, as it may possibly represent the Lower 
 Kittanning bed. 
 
 There may have been other bedsof coal passed through 
 by the drill in the well from which this section is taken, 
 since it is seldom that drillers for oil and gas exercise much care in ex- 
 amining the drillings for coal. 
 
 Fio. 111. — Section 
 under Charles- 
 ton, W. Va. 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 137 
 
 Section at mouth of Lick Run, near Charleston , West Virginia . — Neur 
 the mouth of Lick Run, 2 miles south of Charleston, a well was 
 bored for gas, by Mr Hulings, and from the super- 
 intendent, Colonel Jordan, I obtained the following 
 52 ’ record (Fig. 112) by combining it with the 70 odd 
 feet of rocks exposed above the mouth of the bor- 
 ing : 
 
 ,, - 
 
 eo’ At mouth of Lick Bun, two miles eCbme Charleston , Kanawha 
 County, West Virginia. 
 
 245 * 
 
 195 
 
 Fin. 112.— month 
 of Lick Run, two 
 miles above Charles- 
 ton, W.Va. 
 
 [See map, T f.] 
 
 Feet. 
 
 1. Coal, Upper Freeport 
 
 2. Shales 
 
 3. 
 
 4. 
 
 5. 
 
 Concealed 
 
 Sandstone, massive ... 
 Coal, Lower Freeport . 
 Shales and concealed 
 Blue slate 
 
 7 I 
 
 20 y 
 
 25 1 
 
 ( Blue sandstone, hard . . 51/ ] 
 j Slate and sandstone. .. 6' j 
 
 Sandstone, Freeport { Sandstone, hard 73' > . . . . 
 
 | Slate 21' I 
 
 1 Sandstone, hard 94' j 
 
 :i 
 
 Slate, blue 
 
 Sandstone 
 
 Slate 
 
 Sandstone, white 
 
 Sandy shale, dark blue 
 
 White pebbly sandstone, top of No. XII. 
 Total 
 
 Feet. 
 
 3 
 
 52 
 
 3 
 
 €0 
 
 245 
 
 33 
 
 50 
 
 32 
 
 15 
 
 195 
 
 Colonel Jordan states that no particular search 
 was made for coal here, and hence several beds may 
 have been passed unnoticed. It is also possible that 
 the top of No. XII is placed about 100 feet too low 
 by the section above, since the ordinary driller fre- 
 quently neglects to note changes in the character of 
 the strata through which the drill passes; hence it 
 is quite probable that a considerable thickness of No. 
 13, which the drillers called u sandy shale,” may have 
 been really the top portion of the No. XII series. 
 
 The Freeport sandstone, No. 8, exhibits an unusual 
 development here, and it is possible that the lowest 
 division included in No. 8 is not really a member of 
 this stratum, but belongs lower in the series. 
 
 No. 10 is probably a representative of the Kittan- 
 ning sandstone. 
 
138 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. G5. 
 
 Section at Dickinson salt works , Kan ay ha County , West Virginia . — 
 In the vicinity of Malden, 6 miles above- Charleston, the rapid rise of 
 the strata on the northwestern slope of the Brown stown anticlinal has 
 
 brought nearly all of the Lower Coal Measures to 
 the surface, and the rest of the column is supplied 
 from the records of the Edwards gas well No. 2, at 
 the Dickinson salt works. The combined section 
 reads as follows (Fig. 113): 
 
 Dickinson salt works , Kanawha County , W st Virginia. 
 
 [See map, T f.J 
 
 1. Coal, Upper Freeport, slaty 
 
 2. Shales 
 
 3. Sandstone, massive 
 
 4. Shales 
 
 5. Coal, Lower Freeport.. 
 
 6^ Shales 
 
 7. Sandstone, massive 
 
 8. Sandy shales, with iron ore nodules . 
 
 9. Concealed 
 
 10. Sandstone, massive 
 
 C Coal, slaty O' 5" ) 
 
 11. Coal, Upper Kittanning < Slate, black 0' 11" > 
 
 ■ (Coal 2' 1") 
 
 12. Fire clay, sandy 
 
 13. Concealed * 
 
 14. Sandstone, massive 
 
 it; rw 5 Cedar Grove ( 
 
 Coal \ Middle Kittanning 5 
 
 16. Concealed, and shales 
 
 17. Sandstone 
 
 18. Sandy shales 
 
 19. Limestone, siliceous, Campbell’s Creek 
 
 20. Shales and sandstone 
 
 21. Coal, Campbell’s Creek, 
 Lower Kittanning . . . 
 
 22. Shales 
 
 23. Sandstone, massive 
 
 24. Concealed in bore hole 
 
 25. Sandstone, white 
 
 26. Shales 
 
 27. White sandstone, top of Ko. XII. ' 
 
 ( Coal 2' 0") 
 
 Shales 1' 2" 
 
 Coal 0' 4" 
 
 Fire clay and shales 1' 10" 
 Coal and slate O' 8" 
 
 Coal O' 10" 
 
 1 Slate 0' 2" 
 
 Coal V 8" 
 
 j Fire clay and shales 7' 0" 
 
 Coal, slaty 0' 6" 
 
 I Fire clay 1' 2" 
 
 [Coal (f 3" J 
 
 ( Cedar Grove 
 
 } Middle Kittanning. 
 
 ( Coal, slaty 1' 6" 
 
 I Rock O' 6" 
 
 { Coal 1' 6" 
 
 | Shale 0' 6" 
 
 [Coal, slaty 1' 6" 
 
 ore nodules 
 
 Ft. Ft. in. 
 4 
 5 
 
 65 S 85 
 15 
 
 5} 
 
 65 
 
 3 
 
 20 
 50 j 
 
 143 
 
 2 ? 
 
 55 V 187 
 130 ) 
 
 151 
 
 it 
 
 35 
 
 0 8 
 
 63 
 
 17 7 
 
 SI 
 
 132 
 
 Total. 
 
 641 2 
 
 This section would seem to confirm the statement 
 made in connection with the Lick Run boriug, viz, 
 that a part of the last interval given there should 
 more properly be credited to No. XII, the next 
 series below the Lower Coal Measures. 
 
 The Campbell’s Creek, or Lower Kittanning coal, 
 is here very much split up with slate and shales, 
 
 fig. 113. — Sec ti o n at but on the Malden side of the Kanawha it is a good 
 KanaTha County^wl bed, from which 4 to 6 feet of coal is obtained with 
 
 Va ‘ 
 
 only the two parting slates. 
 
 This is the type locality of the Campbell’s Creek limestone No. 19. 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 139 
 
 Section near Brownstown , West Virginia . — In r the vicinity of Browns* 
 town and near the Burning Spring, 9 miles ^^e^Gharleston, another 
 gas well was drilled (Edwards No. 1) and its record 
 combined with the surface exposures in that vicinity 
 gives the following succession (Fig. 114) : 
 
 Near Broivnstoicn, three miles south from Malden. 
 
 [See map, T f.] 
 
 < 37 ^ 
 
 2 ' 6 " 
 
 1. Coal, Upper Freeport, slaty 
 
 2. Concealed 
 
 3. Sandstone, massive, gray 
 
 4. Shales, and concealed 
 
 5. Sandstone, massive, gray 
 
 6. Sandy shales, and concealed 
 
 7. >andstone, gray, micaceous 
 
 8. Concealed 
 
 9. Coal (Cedar Grove), Middle Kittanning. 
 
 10. Concealed, and sandstone 
 
 ( Lower Kit- 1 Coal 
 
 12. Coal. < > Shales and sandstone ..20' 0" 
 
 j Campbell s f Pnal 9 , 
 
 [ Creek. J Coal Z 4 
 
 13. Shales - 
 
 14. Sandstone, massive 
 
 15. Concealed *. 
 
 16. Coaly shale 
 
 17. Fire clay, sandstone, and concealed 
 
 18. Coal, Brownstown 
 
 19. Shales 
 
 20. Sandstone, massive 
 
 21. Sandy shales and flaggy sandstone 
 
 22. Limestone, siliceous, Ferriferous 
 
 23 Shales, sandy 
 
 24. Slate, black. 
 
 25. Shales 
 
 26. Sandstone, and concealed 
 
 27. Coal, Clarion (Eagle) 
 
 28. Sandstone 
 
 29. Slate, gray 
 
 30. Sandstone, gray 
 
 31. Slate, dark 
 
 32. White sandstone, top of No. XII. 
 
 It. in. 
 
 10 
 
 95 
 
 30 
 
 40 
 
 25 
 
 160 
 
 15 
 
 Ft. in. 
 5 
 
 )> 375 
 
 Total .. 
 
 3 4 
 
 100 
 
 24 10 
 
 74 
 
 2 
 
 70 
 
 1 
 
 45 6 
 
 3 
 
 801 8 
 
 100 
 
 741 
 
 The only part of this series dependent on the bore 
 hole record is the last 100 feet, or that from the 
 Clarion coal down, the rest of it all being exposed 
 above the bed of the Kanawha in the 
 region of Brownstown. 
 
 By comparing this with the Charles- 
 ton section (Fig. Ill) it will be seen 
 that the whole column has thickened 
 southward at the rate of about 25 feet 
 to the mile. It will also be observed 
 that with this thickening a new coal, 
 the Brownstown, makes its appear- 
 ance in the series. This is one of a 
 local group of two or three coals which 
 appear in the column of rocks around 
 the southeastern margin of the coa 
 field between the Lower Kittanning bed and the Ferriferous limestone, 
 which would seem to be represented by No. 22 of the section. These coals 
 are of little economic importance, as they are usually thin and slaty. 
 
 
 Fig. 114. — Section near Brownstown, three 
 miles south from Malden, W. Va. 
 
140 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. G5. 
 
 Section at mouth of Armstrong Creek, on the Big Kanawha River , West 
 Virginia .— At the mouth of Armstrong Creek, 25 miles south from 
 Charleston, the whole column of the Lower Coal Measures is above 
 water level, and a high point almost vertically above 
 the Kanawha Kiver catches the top members of the 
 same, so that here a very fine exposure of the series 
 gives the following structure (Fig. 115) : 
 
 Mouth of Armstrong Creek, on the Big Kanawha River. 
 
 [See map, U g.] Ft. 
 
 1. Coal. Upper Freeport 
 
 2. Sandstone, and concealed 170' 
 
 3. Sandstone, massive 60 
 
 4. Concealed, and sandstone 115 
 
 5. Limestone, siliceous 2 
 
 zo' 
 
 zh r 
 
 -- — - 
 
 BrCTftyCWSBBBp' 
 
 Ft. in. 
 3 
 
 372 
 
 Coal 
 
 ... 6" 
 
 Shale... 
 
 ... 8" 
 
 Coal. — 
 
 ... 5" 
 
 Shale 
 
 ... 6" 
 
 Coal 
 
 ... 4" 
 
 2 5 
 
 8. Fire clay, and concealed. 
 
 9. Sandstone, massive . 
 
 5] 
 
 20 
 
 37i' 10. Shales, concealed, and sandstone 20 
 
 20 
 
 11. Concealed, 
 
 12. Sandstone and shales 20 >165 
 
 13. Sandstone, massive 25 J 
 
 14. Shales, and concealed 20 I 
 
 15. Sandstone 25 | 
 
 H 
 
 6 " ) 
 
 V 8 " 
 
 0 " | 
 0" I 
 
 0" I 
 
 5" f 
 i" C 
 
 16. Sandy shales 
 
 Coal 1' 
 
 Slate 0' 
 
 Coal O' 
 
 Sandy shales 12' 
 
 Coal, “ Peerless ” 2' 
 
 . Shales, bluish. 15' 
 
 17. Coal, Lower Eittan- \ Coal, sulphurous O' 
 
 ning \ Slate 0' 
 
 Coal 0' 6" 
 
 Coal, splint O' 11" 
 
 Parting O' £" 
 
 I Coal 0' 7" I 
 
 | Slate O' I 
 
 [ Coal 2' 10" J 
 
 18. Fireclay - 
 
 19. Sandstone and shales . 
 
 [Coal V 0"1 
 
 Shale 2' 6" | 
 
 20. Coal, Browns- ! Coal O' 10" 
 
 town ] Shales and 
 
 sandstone . .15' 0" 
 
 1 Coal 1' 2" 
 
 10J 
 
 z°' 
 
 l2'6foS| 
 
 15’ 
 
 ft" 
 
 40’ 
 
 36 
 
 21. Concealed, and sandy shales. 40 ) 
 
 22. Limestone, siliceous, Ferriferous 1 > 
 
 23. Shales 10) 
 
 Coal 0' 8"] 
 
 Shales 1' 
 
 Coal, slaty ... 0' 
 
 20 6 
 
 51 
 
 24. Coal, Clarion 
 
 < Shales, sandy. 20' 
 < Ea * le > | Coal.......... 0' 
 
 " 
 
 :: 
 
 I Shales 0' 8" I 
 
 [Coal 2' 10" J 
 
 25. Shales and sandy beds 
 
 26. Coal. Little Eagle - 
 
 27. Fire clay and shales 
 
 I3l' 
 
 30. Limestone, fossiliferous, Eagle . . . 
 
 31. Dark shales, fossiliferous . . 
 
 32. Shales, sandstones, and concealed. 
 
 33. Bituminous shale 
 
 35. Limestone, siliceous •>.. 
 
 36. Shales, sandstone, and concealed r -.. 
 
 37. Sandstone, massive, top of No. XII. 
 
 
 26 
 
 
 20 
 
 - 5 1 
 
 1 
 
 1° 
 
 > 55 
 
 40 : 
 
 1 
 
 1 
 
 5 ] 
 75 J 
 
 > 80 
 
 
 2 
 
 30 ) 
 
 l 
 
 1 
 
 »131 
 
 ioo 5 
 
 I- ‘ 
 
 Total. 
 
 1, 006 7 
 
 Fig. 115. — Section at mouth of Armstrong 
 Creek, en the Big Kanawha Uiver. 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 141 
 
 Here both the Lower Kittanning and the Clarion coals show in their 
 structure the eifect of the general thickening up of the whole column 
 of rocks. Three miles north from this, the Clarion or Eagle coal is a 
 good bed, which, with its partings of slate, is only 4J feet thick, but the 
 partings gradually thicken and new ones come in till the structure 
 shown in No. 24 is obtained. 
 
 A small coal which has been termed the Little Eagle comes into the 
 section in this region, and seems to have a wide distribution around 
 the southern margin of the coal field. It is a very pure coal and may 
 be a lower member of the Clarion bed. 
 
 The Eagle limestone, No. 30, was named from a mining village 3 
 miles below the locality of this section, where it is finely exposed in the 
 cuts of the Chesapeake and Ohio Railroad. It and the shales below it 
 are crowded with the Lower Coal Measures fossils, the general facies of 
 the fauna being very similar to that found in connection with the Fer- 
 riferous limestone in western Pennsylvania, but the general section for- 
 bids the supposition that it is identical with the latter. At one time I 
 entertained the idea that it might be the representative of the Putnam 
 Hill limestone, of Ohio, but a closer study of the Ohio section renders 
 that hypothesis untenable, since the Putnam Hill bed belongs above 
 the Clarion coal and not below, as does the Eagle limestone. 
 
 No. 33 is a very bituminous shale, since lubricating oil was once 
 manufactured therefrom, and it may possibly represent the Brookville 
 coal of Pennsylvania. 
 
 A comparison of this section with those on the other side of the Ap- 
 palachian basin at Buchtel (106) and Shawnee (105) will show the 
 wonderful expansion of these beds from 175 feet at the latter localities 
 to a thickness of more than 1,000 feet at Armstrong’s Creek, and the 
 same thing is shown graphically in map, Section C. That such a great 
 expansion of these measures should show only the same number of 
 workable coal beds as the section at Shawnee was hardly to be expected, 
 but it is true beyond question. The coal beds themselves give evidence 
 of this great expansion of the general column in the slates and other 
 impurities with which they are interstratified. 
 
 The interval (165 feet) which here separates the Middle and Lower 
 Kittanniug coal beds appears excessive, since it is only 100 feet a few 
 miles below, but there can be very little doubt of the figures given, and 
 as there are no coal beds between Nos. 7 and 17, it is evident that No. 
 7 must be the Middle Kittanniug. 
 
 The top member of the Pottsville conglomerate is in the bed of the 
 Kanawha, where the section shown in Fig. 115 ends. 
 
142 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section at Guyandotte Mountain , Raleigh County , West Virginia . — 
 That the Lower Coal Measures keep their greatly expanded measure- 
 ment on south westward from the Kanawha River is shown by the fol- 
 lowing section (Fig. 116) made by Captain Miller, chief engineer of the 
 Trans-Flat-Top Land Association. It begins at the summit of Guy- 
 andotte Mountain, Raleigh County, West Virginia, 
 and was measured along the turnpike eastward to the 
 foot of the mountain : 
 
 Guyandotte Mountain , Raleigh County , West Virginia. 
 
 [See map, W g.] 
 
 1. Upper Freeport coal (absent). 
 
 2. Massive sandstone 
 
 3. Shales 
 
 4. Coal, Lower Freeport . . ^ Slate 
 
 5. Shale 
 
 6. Coal, Winnifrede Slate 
 
 ( Coal 
 
 < Slate 
 
 L Coal 
 
 3' 10" i 
 
 . 0' 1"> 
 
 O' 9") 
 
 { Coal 
 
 2' 
 
 5") 
 
 1 Shale 
 
 12' 
 
 2" 1 
 
 | Coal 
 
 1' 
 
 3" 1 
 
 Slate 
 
 0' 
 
 2" )■ 
 
 1 Coal 
 
 2' 
 
 3'' 1 
 
 ! Slate 
 
 O' 
 
 1" ! 
 
 [Coal 
 
 O' 
 
 1"J 
 
 Ft. in. Ft. in. 
 
 83 
 
 15 
 
 7. Sandstone, hard, gray 28 
 
 8. Shale 81 
 
 9. Sandstone 8 
 
 10. Shale 14 
 
 11. Sandstone, hard, grav 53 
 
 12. Shale .1 32 
 
 13. Sandstone, shaly 24 
 
 14. Shale, yellowish 7 
 
 247 ' 
 
 Coal 
 
 0' 7 " 
 
 Slate 
 
 0' 1 " 
 
 Coal 
 
 0' 9 " 
 
 Slate 
 
 0' 0*" 
 
 Coal 
 
 1' 1 " 1 
 
 Slate 
 
 0' 4 " 1 
 
 Coal 
 
 v H"J 
 
 
 67 
 
 16. Sandstone, soft, yellow 19 
 
 17. Coal 0 
 
 18. Fireclay 1 
 
 19. Shales, yellowish 36 
 
 21/ 
 
 20. Coal, Browns* 
 town 
 
 70 
 
 26 ' 
 
 f Coal O' 1' 
 
 < Fireclay. 2' 0' 
 (Coal...'.. 1' 1") 
 
 21. Fire clay 0 
 
 22. Sandstone, soft, yellow 15 
 
 23. Sandstone, hard, gray 22 
 
 24. Sandstone, soft, yellow, micaceous 21 
 
 25. Shales, yellowish 67 
 
 26. Coal 0 
 
 27. Fire clay 1 
 
 28. Slate, black 16 
 
 29. Sandstone, soft, yellow 35 
 
 30. Shales, yellow 39 
 
 31. Coal, Eagle 
 
 ZO& 
 
 [Coal 
 
 1' 3" 
 
 Slate 
 
 4' 0" 
 
 Fire clay . . 
 
 2' 0" 
 
 Coal 
 
 0' 1" 
 
 Clay 
 
 0' 3" 
 
 Coal 
 
 0' 9" 
 
 Clay 
 
 0' 2" 
 
 Coal 
 
 0' 1" 
 
 Clay 
 
 1' 0" 
 
 [Coal 
 
 0' 1" 
 
 Fig. 116. — Section at Gnyandotte Mountain, 
 Raleigh County, W. Va. 
 
 32. Sandstone, hard, gray 13 
 
 33. Sandstone, soft, yellow 33 
 
 34. Coal, Little Eagle 
 
 35. Fireclay 1 
 
 36. Shales, sandy, yellow 46 
 
 37. Sandstone, soft, yellow 70 
 
 38. Shales, sandy, yellowish 58 
 
 39. Sandstone, flaggy 7 
 
 40. Shales, yeilow 26 
 
 41. Pebbly sandstone, top of Xo. XII. 
 
 4 8 
 43 
 
 18 5 
 
 247 
 
 1 
 
 56 3 
 
 “j 
 
 3 2 
 
 2 \ 217 
 
 4 . 
 
 0 8 
 
 0 3 
 
 Total. 
 
 >2u8 
 
 855 5 
 
WHITE. J 
 
 THE LOWER. COAL MEASURES. 
 
 143 
 
 It is possible that the horizon of the Upper Freeport coal should have 
 been placed higher than the section shows, since the coal is not present 
 and the place given it is only a surmise. 
 
 Section near Oceana , Wyoming County , West Virginia . — In the vicinity 
 of Oceana, Wyoming County, West Virginia, and the neighboring re- 
 gion, the Lower Coal Measures present the following 
 structure (Fig. 117): 
 
 Wyoming County , West Virginia. 
 
 [See map, W f.] 
 
 1. Upper Freeport coal (not seen) 
 
 2. Sandstone, and concealed . 
 
 ( Coal 
 
 Ft. in. 
 
 O' 
 
 \\v 
 
 ■ *.*■■* *-> - 
 
 * ♦ ♦ r * • 
 
 3. Coal, Lower Freeport . . 
 
 1" 
 
 Shale O' 4" 
 
 Coal 0' 10" . 
 
 Bony coal 0' 4" | 
 
 Coal 2' l".j 
 
 4 Sandstone, and concealed 
 
 5. Cannel slate mixed with coal, Upper Kittanning. 
 
 6. Concealed „ 
 
 7. Sandstone, massive 
 
 15S 1 
 
 8. Coal, Middle Kit- 
 tanning 
 
 ( Coal 
 
 1' 
 
 6" ) 
 
 < Shale 
 
 0' 
 
 5" > 2 
 
 (Coal 
 
 0' 
 
 8" 5 
 
 Shales and sandstone 
 
 
 20 
 
 ^ f Coal, good 
 
 2' 
 
 6" ) 
 
 1 Shale, gray 
 
 0' 
 
 2*" 
 
 i Coal 
 
 0' 
 
 34" > 4 
 
 | Shale, gray 
 
 0' 
 
 10" I 
 
 1 [Coal 
 
 0' 
 
 9" J 
 
 
 fe' a ’ 
 
 100 * 
 
 n'2? 
 
 wa 11 
 
 2 A$* 
 
 40 
 
 ZO 
 
 7V 
 
 9. Concealed, and sandstone 20 
 
 10. Coal 0 
 
 11. Fire clay and shales 5 
 
 12. Sandstone, massive 50 
 
 13. Shales, dark, slaty 10 
 
 Coal.. 1' 0") 
 Slate. 10' 
 
 Coal.. 1' 
 
 Slate, 
 
 dark. 
 
 Coal . . 
 
 Slate . 
 
 I Coal . . 
 
 I Slate . 
 
 I Coal . . 
 
 15. Massive sandstone ... 
 
 16. Concealed 40 
 
 17. Shales 20 
 
 tfitf 
 
 7Q 
 
 5 ft 
 
 65’ 
 
 14. Coal, Lower 
 Kittan- 
 ning 
 
 O' 
 
 8 " 
 
 0 ' 6 " 
 
 V 2" f 
 0' 4" | 
 4' 0" 
 
 5' 3" I 
 0' 10" J 
 
 100 
 
 2d 
 
 18. Coal, Browns- 
 
 20 . 
 
 Coal, Eagle 
 (Clarion) 
 
 f Coal.. 
 
 . 1' 7" 
 
 Slate . 
 
 . 1' 4" 
 
 Coal.. 
 
 . 0' 2" 
 
 Q 1 Sla te . 
 
 . 0' 8" 
 
 8 '-» Coal.. 
 
 . 0' 4" ; 
 
 ’ ' 1 Slate . 
 
 . 0' 4" | 
 
 Coal.. 
 
 . 0' 6" 
 
 1 Slate . 
 
 . 1' 8" | 
 
 1 Coal. . 
 
 . 1' 0" J 
 
 and concealed . . 
 
 C Coal . 
 
 . 3' 4" ) 
 
 < Slate . 
 
 . 0' 4" ) 
 
 •’ (Coal.. 
 
 . 2' 0" j 
 
 21. Concealed, and shales 
 
 22. Coal, Little Eagle 
 
 23. Shales and sandstones 75 
 
 24. Shales, gray, with fossil plants 5 
 
 25. Coal 
 
 26. Concealed, and shales and sand- 
 
 stone 
 
 27. Coal, blossom 
 
 28. Shales 
 
 29. Massive sandstones, top of 
 
 No. XII. 
 
 Total 
 
 bmmm 
 
 Fig, 117.— Section near Oceana, Wyoming 
 County, W. Va. 
 
 Ft. in. 
 100 
 
 155 
 
 3 
 
 2 
 
 70 
 
 > 27 2 
 
 24 9 
 
 160 
 
 7 7 
 
 10 
 
 100 
 
 30 
 
 993 
 
144 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 | BULL. 65. 
 
 No. 20 is known as the “coking coal ” in the Wyoming region, since 
 it has the typical structure of such coal, and looks very much like the 
 same (Eagle) bed on the Kanawha. 
 
 The Little Eagle bed No. 22 is also very good coal here, and its in- 
 terval below the main seam has increased from 20 to 05 feet. 
 
 Section at mouth of Blaine Greek , Lawrence County , Kentucky . — In 
 passing southward up the Big Sandy River, at the 
 southwestern line of West Virginia, the Lower Coal 
 Measures thicken up at about the same rate as they 
 do along the Kanawha, as will be seen from the follow- 
 ing sections. The first one (Fig. 11 8) is from a sur- 
 face measurement, combined with the record of liig- 
 don gas well No. 2, at the mouth of Blaine Creek, JO 
 miles above the mouth of the Big Sandy River, and 
 reads as follows : 
 
 
 
 122 ,* 
 
 Mouth of Blaine Creelc, twenty miles above mouth of Big Sandy 
 Biver, Kentucky. 
 
 [See map, T b.] 
 
 Fig. 118. — Section at 
 mouth of Blaine 
 Creek, Ky. 
 
 1. Coal and black slate, Upper Freeport 
 
 2. Sandstone 
 
 3. Slate, black 
 
 4. Coal, Lower Freeport 
 
 5. Fireclay 
 
 6. Sandstone, white 
 
 7. Sandstone, dark gray 
 
 8. Sandstone, white 
 
 9. Slate, black 
 
 10. Sandstone, dark 
 
 11. Slate, black 
 
 12. Coal, Middle Kittanning 
 
 13. Slate 
 
 14. Sandstone, gray 
 
 15. Slate, black 
 
 16. Sandstone, gray 
 
 17. Coal, Lower Kittanning 
 
 18. Fire clay 
 
 19. Sandstone, gray 
 
 20. Slate, gray 
 
 21. Sandstone, gray 
 
 22. Slate, black 
 
 23. Sandstone, white, top of No. XII. 
 
 Feet. Feet. 
 
 5 
 
 30 > 
 
 50 ( 80 
 
 4 
 7 
 
 45 
 10 
 10 
 15 
 25 
 10 
 
 27 
 
 122 
 
 
 25 
 
 Total. 
 
 218 
 
 521 
 
 For the carefully kept record of this boring I am indebted to Mr. 
 F. H. Oliphant, now the chief geologist of the South Penn Oil Com- 
 pany. 
 
WHITE.] 
 
 THE LOWER COAL MEASURES. 
 
 145 
 
 Section near Old Peach Orchard , Laivrence County , Kentucky. — Id the 
 vicinity of Old Peach Orchard, on the Louisa fork of Big Sandy 
 Biver, Kentucky, the surface measurements, com- 
 bined with the records of oil and gas borings near by, 
 give the following structure (Fig. 119) : 
 
 1:1 
 
 15' 
 
 
 SM 4 ' 
 
 35* 
 
 Near Peach Orchard, Kentucky. 
 
 [See map, V b.J 
 
 Ft. in. Ft. in. 
 
 Upper Freeport coal (absent) 
 
 Sandy shales - 20 
 
 Sandstone and sandy beds 80 
 
 Coal 
 
 f Lower Freeport, or | 
 
 r Coal — 
 
 ...O' 
 
 10" ) 
 
 < Winnifrede, Peach < 
 
 ; Shale ... 
 
 ... 0' 
 
 10" J 
 
 ( Orchard bed - 1 
 
 [Coal .... 
 
 ... 2' 
 
 4" ) 
 
 100 
 
 < 
 
 
 > 137 4 
 
 15. Coal 
 
 >") 
 
 S">— • 
 
 V'S 
 
 4| 
 
 Fire clay, siliceous 2 
 
 Sandy shales 35 
 
 Massive sandstone and sbaly micaceous beds 75 
 
 Blue sandy shales - : 25 
 
 ( Cannel 1' 0" 
 
 Coal, Upper Kittanning< Clay O' 6" 
 
 t Coal, slaty 1' 0" 
 
 Shale and sandstone 10 
 
 Coal - 0 
 
 Sandy shale, blue 8 
 
 Limestone 2 
 
 Sandstone, shaly 12 
 
 ( Coal O' 6" ) 
 
 < Shale 1' 6" V .... 
 
 ( Coal O' 8" ) 
 
 16. Concealed, and shaly sandstone 9 
 
 17. Black slate 4 
 
 18. Coal, splint, Middle Kittanning 
 
 19. Concealed 10 
 
 20. Hard sandstone 70 
 
 21. Blue shale 2 
 
 22. C< al, Lower Kittanning 
 
 23. Shales and fire clay 10 
 
 24. Sandy shale 15 
 
 25. Black shales 115 
 
 26. Sandstone 4 
 
 27. Dark shale 110 
 
 28. White sandstone, top of No. XII. 
 
 Total 634 10 
 
 r* 
 
 2 6 
 32 4 
 
 2 8 
 
 13 
 
 1 
 
 82 
 
 6 
 
 254 
 
 The place of the Upper Freeport coal here is deter- 
 mined with comparative certainty by the massive Ma- 
 honing sandstones, which come in above No. 1, and 
 also by the occurrence of the Mahoning coal, with its 
 characteristic structure, at 235 feet above the Peach 
 Orchard bed, and 135 feet above where the horizon of 
 the Upper Freeport has been placed. 
 
 No. 15 is very probably a “split” from the Middle 
 Kittanning bed, No. 18, and should be regarded as 
 a part of the latter. 
 
 The Lower Kittanning bed, No. 22, is given as re- 
 ported from a bore hole at “ Old” Peach Orchard, by 
 Prof. Shumard, who examined the drillings at the 
 time the boring was made, and the rest of the section 
 F oVd 19 T >S eacb D ()?■ below this is from a deep boring made for gas, about 
 3 miles distant, the record of which was obtained from 
 Mr. F. H. Oliphant, the civil engineer under whose superintendence 
 the deep well was bored. 
 
 Bull 65 10 
 
146 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 There has been much variance of opinion among geologists who have 
 examined the Peach Orchard coal bed as to its horizon in the series, 
 some placing it as far down in the column as the Clarion coal, but this sec- 
 tion shows that it is either the Lower Freeport coal of the Pennsylvania 
 column or else one that is probably a u split” from the 
 latter, viz, the Winnifrede bed of the Kanawha series. 
 
 Section near Warfield , Kentucky . — In the vicinity of 
 Warfield, Kentucky, opposite the line of Logan County, 
 West Virginia, and 60 miles above the mouth of the Big 
 Sandy, the following structure (Fig. 120) is obtained by 
 combining the surface observations with the records of 
 of the Warfield gas wells : 
 
 Warfield, Kentucky, on Tug Fork of Big Sandy Biver. 
 
 [See map, V b.l 
 
 «/ 
 
 Upper Freeport coal (not seen) . 
 Massive sandstone, and concealed 
 
 sa' 
 
 3. Coal, Winnifrede... 
 
 f Coal 
 
 . O' 
 
 5" 1 
 
 1 Sandy shales. . 
 
 .10' 
 
 0" 1 
 
 | Fire clav 
 
 . 2' 
 
 0" 
 
 j Coal, splint 
 
 . 1' 
 
 2" [ 
 
 i Clay 
 
 . 0' 
 
 1 "l 
 
 1 Coal, splint 
 
 . 1' 
 
 4" 
 
 1 Clay 
 
 . 0' 
 
 i"\ 
 
 [Coal 
 
 . 0' 
 
 9" J 
 
 Ft. in. Ft. in. 
 150 
 
 15 0 
 
 
 4. Concealed, and sandstone 25 
 
 5. Limestone, siliceous 4 
 
 6. Shales, sandstone, and concealed 30 
 
 7. Coal, cannel, Upper Kittanning 
 
 8. Sandstone, and concealed 30 
 
 9. Limestone, siliceous I 
 
 10. Sandstone, and concealed 20 
 
 11. Coal, blossom, Middle Kittanning 
 
 12. Concealed, and sandstone 
 
 13. Limestone, siliceous 
 
 14. Sandstone, massive 20 
 
 15. Shale 0 
 
 16. Coal 0 
 
 17. Sandstone and shales 40 
 
 18. Sandstone, massive 10 
 
 ( Coal O' 4" > 
 
 19. Coal, Lower Kittanning < Shale O' 10" v 
 
 ( Coal 4' 0" S 
 
 20. Concealed, and sandstone 
 
 21. Limestone, siliceous 
 
 22. Shales and sandstones to top of Xo. XU 
 
 Total 
 
 45 
 
 2 
 
 320 
 
 787 6 
 
 Some have supposed that No. 3 of this last section is 
 identical with the Peach Orchard bed, but it seems to 
 occupy a horizon a few feet below the latter, and I have 
 therefore referred it to the Winnifrede bed 
 of the Kanawha column. 
 
 No. 19, which is locally known as the 
 “ Warfield” coal, is the same one as No. 22 
 of Section 119, and the representative of the 
 Lower Kittanning bed. 
 
 The u siliceous” limestones, Nos. 13 and 
 21, may possibly represent the Campbell’s 
 Creek and Ferriferous beds respectively. 
 
 Fig. 120. — Section at Warfield, Ky., 
 on Tug Fork of Big Sandy Biver. 
 
WHITE. J 
 
 THE LOWER COAL MEASURES. 
 
 147 
 
 Section on Tut/ Fork of Big Sandy River , Logan County , West Virginia . — 
 ^Near the mouth of Kuox Creek, at the southern edge of Logan County, 
 50 miles by the river above Warfield, the following section 
 (Fig. 121) was constructed on the West Virginia side of 
 Tug River, by adding to the upper portion of the section 
 there the part which has been removed by erosion: 
 
 300* 
 
 
 m 
 
 
 100 ' 
 
 Tug Fork of Big Sandy River , near mouth of Knox Creek , southern edge 
 of Logan County, West Virginia. 
 
 ' 5sT 
 
 vvTvavN' 
 
 40' 
 
 tao’ 
 
 [See map,W d.J 
 
 1. Upper Freeport coal (absent) 
 
 2. Shales and sandstone 
 
 3. Coal, Lower Freeport 
 
 4. Shales and massive sandstone 
 
 5. Coal, Lower Kittanning, large blossom 
 
 6. Sandstone, massive 
 
 7. Shales, sandstone, and concealed 
 
 8. Coal, Eagle, large blossom 
 
 9. Shales and sandstone 
 
 10. Coal, blossom, Little Eagle 
 
 11. Concealed 
 
 12. Sandstone, flaggy 
 
 13. Concealed 
 
 14. Sandstone, gray 
 
 15. Shales, soft, gray 
 
 16. Limestone, blue, impure (Eagle?) 
 
 17. Shales, dark blue 
 
 18. Sandstone 
 
 19. Concealed 
 
 20. Coal 
 
 21. Shales and flaggy sandstone 
 
 22. Slates, dark 
 
 23. Concealed, sandstone, and concealed 
 
 24. Massive coarse sandstone, top of No. XII. 
 
 Total 
 
 Ft. 
 
 
 5(f 
 
 7 ZS' 
 
 Ft. 
 
 100 
 
 300 
 
 6 
 
 40 
 
 180 
 
 5 
 
 55 
 
 2 
 
 140 
 
 1 
 
 75 
 
 l 
 
 85 
 
 Wflf 
 
 CHARACTERISTIC HORIZONS. 
 
 THE UPPER FREEPORT COAL. 
 
 Asmaybeseen by the sections just given, 
 a very important coal bed comes at the 
 summit of the Lower Coal Measures column, 
 and marks the latter off* from the Barrens 
 above. This coal, which was named the 
 Upper Freeport coal by Rogers, has a very 
 wide distribution in the Appalachian field 
 and is the source of much valuable coal 
 and coke. The coal is not entirely persist- 
 ent, however, being frequently too thin to 
 mine, and from large areas it is absent en- 
 tirely, though its horizon in the measures 
 can then still be determined, and generally without much difficulty. 
 The bed is probably more regular and persistent in Pennsylvania than 
 
 Fig. 121.— Section on Tug Fork of Big 
 Sandy River, near mouth of Knox 
 Creek, southern edge of Logau Coun- 
 ty, W. Va. 
 
148 
 
 . THE NORTHERN BITUMINOUS COAL FIELD 
 
 [BULL. 65 . 
 
 in either of the other two States (Ohio and West Virginia), but even 
 there it is not always found in workable condition, being thin or want- 
 ing in some portions of nearly every county where its outcrop extends. 
 
 One of the main features which characterizes this bed is its complex- 
 ity, since it is always separated into two or more benches by divisions 
 of slate. This complexity of structure is illustrated at the type locality 
 (Section G6), and so far as the writer knows it is never entirely absent 
 anywhere in the Appalachian field, whenever the bed is thick enough 
 to mine. These parting slates vary in both number and thickness in 
 different regions, so that there is nothing characteristic about them over 
 the whole field, but yet in any particular district or coal basin their 
 number and position in the bed are quite regular. 
 
 Another peculiarity of the coal is that it nearly always cokes well 
 whenever attaining anything like its normal thickness and hence in 
 several regions is locally known as the “coking veiu.’ 7 There are many 
 districts where this bed will produce coke but little if any inferior to 
 that of the Pittsburgh, in the famous Connellsville basin, and when the 
 latter is exhausted the next source of supply to the Pittsburgh and 
 Pennsylvania region generally must come largely from this horizon. 
 Still another feature of this coal is its tenderness, and by this it can 
 often be distinguished from the very hard Mahoning coal next above 
 (which often rivals this bed in size), since as a rule the coal from the 
 Upper Freeport horizon does not bear much handling without breaking 
 up most of the lumps, although they often come out of the mine with 
 large size. This is true of the bed everywhere in Pennsylvania and 
 West Virginia (except in the southwestern part of the latter State, where 
 it is often a splint coal), and Prof. Orton reports the same thing as char- 
 acterizing it all over the Ohio field. 
 
 There is frequently a layer of impure cannel or highly bituminous slate 
 in the roof of this coal, and in the Great Kanawha region a fine deposit 
 of cannel coal occurs at this horizon. This is true of the Cannelton 
 locality, but whether any of the cannel deposits on Coal River, south 
 from the Kanawha, belong at this same geological level is as yet unde- 
 termined, since the latter have not been sufficiently studied, though the 
 flora would indicate that the Peytona deposit belongs at the horizon 
 of the Upper Kittanning coal. 
 
 The several sections that have already been given (Kos. 50-121), in- 
 dicate the structure of the Upper Freeport bed in many regions, but 
 there remain others where it is equally important, and some of these 
 will now be given. 
 
 Section at McCoy shaft, near Oallitzin, Cambria County, Pennsylvania . — 
 Some large coke plants have recently been put into operation on this, 
 bed along the line of the Pennsylvania Railroad and its branches on 
 the summit of the Alleghany Mountains in Cambria and Clearfield 
 
WHITE.] THE UPPER FREEPORT COAL. 149 
 
 Counties. At the McCoy shaft, near Gallitzin, the coal has the follow- 
 ing structure, according to the superintendent’s statement: 
 
 • Ft. in. 
 
 Black slate and bone coal 0 8 1 
 
 Slate, gray 0 2 I Ft - in * 
 
 Coal 1 0 > 6 5 
 
 Slate 0 3 | 
 
 Coal 0 4 J 
 
 Section near eastern end of old Portage Railroad tunnel , at Gallitzin , 
 Pennsylvania. — Near the eastern end of the old Portage Railroad tun- 
 nel, at Gallitzin, the coal is well exposed, and there shows as follows : 
 
 Coal 
 
 Dark slate and bony coal 
 
 Coal 
 
 Slate, gray 
 
 Coal 
 
 Slate and slaty coal 
 
 Ft. in. 
 
 0 4 ^ 
 
 0 2 j 
 
 3 0 I Ft * in - 
 
 0 2 
 
 1 2 
 0 10 J 
 
 > 5 8 
 
 According to Messrs. Chance and Platt, this coal is but poorly repre- 
 sented in the present mining regi< ns of Clearfield and Jefferson Coun- 
 ties, Pennsylvania, but it is possible, as already suggested in connec- 
 tion with section 88, that in some cases, at least, the Upper Freeport 
 coal may have been erroneously referred to the horizon of the Lower 
 Freeport. 
 
 Section at Mount Equity mine , Bedford County , Pennsylvania . — In the 
 Broad Top field this coal is finely developed in Bedford County, where 
 it is known as the “ Kelly seam,” and exhibits the following structure at 
 the Mt. Equity mine, according to Stevenson, Report T 2 , Second Geo- 
 logical Survey of Pennsylvania, page 62 : 
 
 Ft. in. 
 
 Coal 2 1 
 
 Parting 
 
 Coal 0 7 
 
 Parting Ft. in. 
 
 Coal 1 2 7 2 
 
 Parting 
 
 Coal 1 0 
 
 Clay 2 0 
 
 Coal 0 4 . 
 
 Although this bed is so well developed in Bedford County, yet when 
 followed northward into Huntingdon, only 10 miles distant, it thins 
 away to only 1 foot or even less. 
 
 Followed southward from Cambria County along the Alleghanies, 
 this coal becomes quite thin and slaty in Somerset, and where the bed 
 enters Maryland near the northern end of the Georges Creek basin, it 
 is only 8 to 4 feet thick and quite slaty, there being a layer of bony, 
 worthless coal, 1 foot thick, just above the middle. 
 
150 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 (BULL. 65 . 
 
 This poor condition of the bed seems to be maintained southward 
 along the Georges Creek basin to Piedmont (Section 92) and up the 
 North Potomac (Section 93) to near its source (Section 94) before the 
 coal becomes valuable again, since there the whole bed thickens up to 
 8 feet, and is extensively mined at Thomas, on the West Virginia Cen- 
 tral Railroad, in spite of the fact that 2 feet of bony, worthless coal still 
 remains near the center of the bed. 
 
 In the Ligonier basin of Westmoreland and Fayette Counties, Penn- 
 sylvania, Prof. Stevenson reports this bed of inferior quality, being 
 filled with knife edges of slate and containing too much sulphur for the 
 manufacture of coke, though it often has a good thickness. This con- 
 dition of affairs is continued southward along the Ligonier basin into 
 Preston County, West Virginia, until we begin to approach the vicin- 
 ity of Cheat River, when a great change takes place in the character 
 of the coal, the sulphur and thin slates disappearing and the whole be- 
 coming a most valuable coking coal. 
 
 Section at Posters bank , near Masontown , Preston County , West Vir- 
 ginia. — The section at Mr. Posten’s bank, 2 miles from Masontown, 
 Preston County, shows the following structure : 
 
 Ft. in. 
 
 Coal, slaty 1 3 ^ 
 
 Coal, good 3 0 I 
 
 Slate, gray 0 3 ! ^ m * 
 
 Coal, good 1 3 > y 7 
 
 Shale 0 10 | 
 
 Coal, good 3 0 j 
 
 This is near the center of the basin, and the coal is there thicker 
 than the average. 
 
 Section at Hartleys bank , near Masontown , Preston County , West Vir- 
 ginia . — The following from the side of the trough near Masontown, at 
 Mr. Hartley’s bank, will better represent the average thickness of this 
 coal in the Preston basin : 
 
 Slaty coal.. 
 Coal, good.. 
 Shale, gray 
 Coal, good.. 
 Shale, gray 
 Coal, good. 
 
 Ft. in. 
 
 0 2 I Ft - in - 
 
 1 3 > 8 7 
 
 1 0 
 
 1 6 , 
 
 The first parting below the top is usually called the “little” slate, 
 while the next one is known as the “ big ” slate. 
 
 This is the same coal that has long been coked for the manufacture 
 of iron at Irondale, Preston County, and also near Austin, on the Balti- 
 more and Ohio Railroad. At both of these localities the coal below 
 the “ big ” slate is not taken out on account of the expense of mining 
 the latter. 
 
 Southward from the Baltimore and Ohio Railroad this bed again 
 splits up with numerous slate partings, and when it comes out to day- 
 
WHITS.] 
 
 THE UPPER FREEPORT COAL. 
 
 151 
 
 light, on the Valley River, at Philippi, the coal is 4 feet thick, but so 
 slaty as to be almost valueless, and only 20 to 25 feet above the Lower 
 Freeport coal. 
 
 Section at Wilson's mine , Roaring Greek , Randolph County , West Vir- 
 ginia. — South ward from Philippi it increases in thickness, and when we 
 come to the eastern side of the Belington basin the bed has a total 
 height of 10 to 15 feet, and is locally known as the Roaring Creek vein. 
 Its structure there is shown by the following section at Mr. William 
 Wilson’s mine, in the northern edge of Randolph County, and about 1 
 mile east from the Valley River, at the mouth of Roaring Creek : 
 
 Coal, slaty, impure ... 
 
 Shales, dark 
 
 Coal, “ upper bench ” 
 Slate and bony coal... 
 
 Coal, “breast” 
 
 Slate, gray 
 
 Coal, “mining ply” . 
 
 Clay and slate 
 
 Coal, “ bottom,” slaty 
 
 Ft. in. 
 
 1 6 
 2 0 
 2 8 
 1 3 
 
 3 i y 
 0 6 
 1 8 
 
 0 4 
 
 1 0 j 
 
 Feet. 
 
 14 
 
 At some localities the u bottom ” and u mining ply ” benches form one 
 layer of coal 3 to 4 feet thick, but as a rule the “ bottom ” portion is 
 slaty and worthless, while the u mining ply” and the u breast” layers 
 furnish very good fuel, the “ upper bench” being frequently slaty and 
 otherwise impure. 
 
 Followed still farther southward along the eastern side of the 
 Appalachian field, through Randolph, Upshur, Lewis, Webster, Nich- 
 olas, Fayette, Kanawha, Lincoln, Cabell, and Wayne Counties, West 
 Virginia, this coal bed presents the features shown in the sections given 
 
 below. 
 
 Section on Stone Goal Run , TJpshur County , West Virginia. — In Upshur 
 County, 10 miles west from the Roaring Creek region, the Upper Free- 
 port coal is exposed on Stone Coal Run, a tributary of the Big Sandy, 
 which empties into the Buckhannon River. Here the following struct- 
 ure is visible : 
 
 Ft. in. 
 
 Black slate 
 
 Coal 
 
 Bony coal . . 
 
 Coal 
 
 Black slate 
 
 Coal 
 
 Gray slate. 
 
 Coal 
 
 •Slate, dark 
 
 Coal 
 
 Slate, dark 
 Coal, slaty. 
 Slate, gray 
 Coal 
 
 6 
 
 0 
 
 8 
 
 0 
 
 0 
 
 0 
 
 6 
 
 r> 
 
 4 
 
 10 
 
 5 
 
 5 
 
 6 
 
 Ft. in. 
 14 
 
 i 0 
 
 V, rO 
 
 f a 
 
 
 Ft. 
 > 22 
 
 7 4 
 
152 THE NORTHERN BITUMINOUS COAL FIELD. [bum,. 65. 
 
 This is the locality of the celebrated u 22-foot” coal bed of Upshur 
 County. The detailed structure above given does, indeed, exhibit a 
 bed of this enormous thickness, but it is so split up with slate as to be 
 practically worthless. 
 
 Section on the Buckhannon River , Up liur County . West Virginia. — Still 
 further west from this, on the main Buckhannon Biver, one-fourth of a 
 mile above Grassy Run and 9J miles from Buckhannon town, in a cut 
 on the West Virginia and Pittsburgh Railroad, the following section is 
 exhibited : 
 
 Massive sandstone (Lower Mahoning) 
 
 
 
 Feet. 
 
 f Cannel slate 
 
 12' 
 
 0"1 
 
 
 1 Coal 
 
 2' 
 
 0" 1 
 
 
 Upper Freeport coal.. <( , 
 
 | Shale 
 
 2' 
 
 0" [ 
 
 .... 17 
 
 f Coal 
 
 V 
 
 0"J 
 
 
 Gray shale 
 
 
 
 .... 3 
 
 Concealed 
 
 
 
 .... 10 
 
 Massive sandstone in bed of Buckhannon River 
 
 .... 5 
 
 Here the coal has almost entirely disappeared in the great mass of 
 cannel slate at the top, which, of course, contains a large quantity of 
 bituminous matter. 
 
 Section at Lloyd Wamsley’s bank. Upshur County , West Virginia. — About 
 10 miles south from the last locality we come to an area of this coal be- 
 tween the main Buckhannon River and its middle fork, where it has 
 regained a structure more nearly normal, viz: 
 
 Ft. in. 
 
 Cannel slate 0 7 
 
 Coal 2 7 
 
 Slate, black 0 4 
 
 Coal 0 8 
 
 Shale, gray 0 8 
 
 Coal, soft .. 1 7 
 
 Mr. Bryan's bank , one half mile northwest, exhibits the following: 
 
 Ft. in. 
 
 Cannel slate 0 6 
 
 Coal 2 0 
 
 Bony coal 0 6 
 
 Coai 3 0 
 
 Section at Current’s farm , Upshur County, West Virginia. — A few miles 
 so uth of this, near the Randolph County line this coal passes into the 
 air on the land of Mr. Current, where it exhioits the following: 
 
 Sandstone . . . 
 
 Coal 
 
 Slate, blue .. 
 
 Coai 
 
 Clay 
 
 Coal 
 
 Sand rock ... 
 Coal, visible 
 
 Ft. in. 
 
 1 oi 
 
 2 2 I 
 0 2 ! 
 0 10 * 
 
 0 G 
 
 1 0 
 1 0 
 
 Ft. in. 
 25 
 
 6 8 
 
WHITE.] 
 
 THE UPPER FREEPORT COAL. 
 
 153 
 
 Section near Hacker's Valley P. 0., Webster County , West Virginia . — 
 Southward from this, through the edge of Randolph, the coal has been 
 eroded by the waters of the Buckhannon, but beyond Helvetia and the 
 Florence Pass we come to an elevated plateau, from which the Buck- 
 hanuon, Little Kanawha, and Holly (a tributary of the Elk) Rivers all 
 take their rise, and here, in Webster County, 7 miles northeast from 
 Hacker’s Valley post-office, we catch an outlier of this coal with the 
 following structure: 
 
 Ft. in. 
 
 Coal, good 1 3 ! Ft - in * 
 
 Bony coal 1 2 j ^ ^ 
 
 Coal, good 2 8 J 
 
 Section on the Little Kanawha River , Lewis County , West Virginia . — 
 About 10 miles northwest from this last locality the same coal exhibits 
 the following structure (according to William S Stevenson) in the hills 
 along the Little Kanawha River, where the left branch of that stream 
 cuts across the panhandle of Lewis County: 
 
 Ft. in. 
 
 Slaty coal 5 O') 
 
 Coal, hard - 2 8 
 
 Slate 0 8 j 9 0 
 
 Coal, softer 1 8 J 
 
 Section on the 'Holly River , Webster County , West Virginia. — In the 
 summit of the hills near Anderson’s mill, on the left branch of Holly 
 Liver, Webster County, we find the Upper Freeport coal with the follow- 
 ing structure on the land of Mr. Marcum Cougar: 
 
 Coal, hard 
 Slate, dark 
 Coal, soft. 
 Bony coal 
 Coal, soft. 
 
 Ft. in 
 3 2 
 
 0 4 
 
 1 4 
 
 0 4 
 
 1 8 
 
 Ft. in. 
 6 10 
 
 Section at Powell Mountain , Nicholas County , West Virginia. — To the 
 southwest from this there are no more openings on this coal until we 
 come to Powell Mountain, in Nicholas County, although a u 7-foot” 
 bed of coal is frequently “reported” in the hills where the Upper Free- 
 port ought to be found. But in Powell Mountain it has been mined 
 for a long time on the Weston and Gauley Bridge turnpike, where it 
 exhibits the following structure: 
 
 Ft. in. 
 
 Coal, blossom ') 
 
 Shales, gray 10 0 j Ft. in. 
 
 Coal, splinty 2 0 ) 14 3 
 
 Black slate • 0 3 | 
 
 Coal, splinty 2 0 J 
 
 Here the character of the coal begins to change to the hard, splinty 
 variety which distinguishes the coals of tiie Kanawha Valley. 
 
154 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section on Stroud Creel', Nicholas County , West Virginia. — A few miles 
 east from this, on the waters of Stroud Creek, this bed shows the follow- 
 ing section on the land of Dr. D. M. Lewis : 
 
 Carmel 
 
 Coal, splint 
 
 Soft coal 
 
 Black slate 
 
 Coal 
 
 Black, coaly slate 
 
 Gray slate 
 
 Coal, soft 
 
 Clay 
 
 Coal, soft 
 
 Slate 
 
 Coal 
 
 Ft. 
 
 in. 
 
 0 
 
 5 1 
 
 . 4 
 
 ° 
 
 . 0 
 
 4 
 
 . 0 
 
 1 
 
 . 0 
 
 6 
 
 . 0 
 
 6 ) 
 
 . 3 
 
 0 
 
 . 1 
 
 10 
 
 . 1 
 
 0 
 
 . 0 10 
 
 . 0 
 
 1 
 
 . 0 
 
 3 J 
 
 Sections on Mumble the peg Creek , Nicholas County , West Virginia. — On 
 Mumble-the-peg Creek, half way between Powell Mountain and Nicho- 
 las Court-House, we find an opening in the Upper Freeport coal on 
 the land of Mr. Herold, where it shows the following structure: 
 
 Coal 
 
 Shales 
 
 Cannel 
 
 Coal, splinty, 
 Slate, black . 
 Coal, splinty 
 
 Ft. in. 
 
 1 61 
 5 0 ‘ 
 0 8 
 2 ' 6 
 1 8 
 2 6 
 
 Ft. in. 
 13 10 
 
 At another bank, 300 yards west from the last, the following is seen: 
 
 Ft. in. 
 
 Coal, blossom 
 Shale, gray.. 
 Bony cannel . . 
 Coal, splinty 
 Slate, black . 
 Coal, splinty 
 
 1 
 
 2 0 I 
 0 6 l 
 2 1 ( 
 0 3 I 
 
 2 6 j 
 
 Ft. in. 
 7 4 
 
 At this locality, as well as iu Powell Mountain and on Stroud Creek, 
 a very good quality of splint coal is obtained from this bed. 
 
 From Nicholas Court-House on southwestward to the Great Kanawha 
 Biver no openings have been examined along the crop of this coal, but 
 at Cannelton, in Fayette County, w r e find it a valuable bed of cannel 
 coal with a thickness of 1£ to 4 feet, while 2 to 2J feet of bituminous 
 coal rests immediately on the latter. 
 
 Two miles below Cannelton, at the mouth of Upper Creek, the bed 
 thickens to 11 feet, but the layers of coa) are so interstratified and 
 diluted with slate and muddy sediment that the whole is worthless. A 
 few miles farther down the Kanawha, at East Bank and Crown Hill, a 
 portion of this great bed becomes the excellent splint coal, 3 to 4 feet 
 
 thick, which is mined at those localities, but farther down this river 
 the bed again becomes impure and remains practically worthless from 
 Coal burg on down until it disappears under the river at Charleston. 
 
WHITE.] 
 
 THE UPPER FREEFORT COAL. 
 
 155 
 
 West from the Kanawha we have no information about this coal until 
 we reach the Guyandotte River in Cabell and Lincoln Counties, but it 
 is possible that some of the Coal River cannel belongs at this horizon.' 
 
 Section on the Guyandotte River , Cabell County , West Virginia . — On the 
 Guyandotte River the Upper Freeport coal rises above water level about 
 two miles above the u Falls Dam.” It is first opened and mined at the 
 mouth of Stone Coal Run, where it exhibits the following structure : 
 
 Coal 
 
 Slate 
 
 Coal 
 
 Slate and bony cannel 
 Coal, visible 
 
 Ft in. 
 
 0 4 " 
 
 0 2 Ft. 
 
 0 7 } 3 
 
 0 9 
 
 1 8 J 
 
 in. 
 
 6 
 
 Another opening a short distance up the run gives the following: 
 
 Massive sandstone 
 
 Cannel slate 
 
 Slate 
 
 Coal, good 
 
 Ft. in. Ft. in. 
 
 25 0 
 
 1 °1 
 
 0 3 > 5 3 
 
 4 0 j 
 
 This latter section very probably belongs immediately on top of the 
 first opening, since the interval between the two banks is concealed. 
 
 The coal is known in this region as the u big bed.” On the Caldwell 
 tract, opposite Camp Branch, this coal exhibits the following section in 
 the bluff overlooking the Guyandotte: 
 
 Sandstone, visible 
 
 Ft. in. 
 10 0 
 
 Coal, 
 
 Upper Freeport.. 
 
 'Coal, slaty.. 
 
 ... V 
 
 0"1 
 
 Coal 
 
 .... V 
 
 6" 
 
 Slate 
 
 .... 0 7 
 
 1" 
 
 Coal 
 
 .... 2' 
 
 0" 
 
 Slate 
 
 .... O' 
 
 2" l 
 
 j Coal 
 
 .... O' 
 
 9" i 
 
 ! Shale 
 
 ... O' 
 
 9" 
 
 Coal 
 
 .... 0' 
 
 8" 
 
 Slate 
 
 .... 0' 
 
 6" I 
 
 tCoal 
 
 
 0"j 
 
 10 5 
 
 As will be perceived, the coal contains much slaty material and the 
 layers of coal themselves are inclined to be bony and impure, approach- 
 ing the type which this bed exhibits in the vicinity of the Kanawha 
 Mining Company’s plant on the Big Kanawha River. 
 
 Sections on Cove Creelc. Wayne County , WestVirginia. — As we pass from 
 the Guyandotte in Lincoln County westward across the divide to the 
 waters of Twelve Pole, a great change takes place in the Upper Free- 
 port bed, and on Cove Creek we find it split into two portions with 30 
 feet of rock between, and the lower bench a fine quality of cannel coal 
 3 to 4 feet thick at some openings. 
 
THE NORTHERN BITUMINOUS COAL FIELD. 
 
 156 
 
 [BULL. C. p 
 
 At another locality the following is seen : 
 
 Ft. in. 
 
 Coal blossom 2 O') 
 
 Shales and sandstone 30 0 j 
 
 Shale O' 6 ,/ 'j > 
 
 Coal, splint 1 ' 8" ! j 
 
 Cannel, good V 4 " f *" 4 1U J 
 
 Coal, bony 1' 4 " j 
 
 m. 
 
 10 
 
 On the opposite side of Cove Creek we see: 
 
 Ft. in. 
 
 Massive sandstone 
 
 Coal 0 6 
 
 Slate 0 4 [ rt - in * 
 
 Coal 1 6 f 5 4 
 
 Cannel 3 0 j 
 
 From this point a belt of cannel coal at the horizon of this bed ex- 
 tends in a general westerly direction nearly across Wayne County, being 
 found on all ot the main branches of Twelve Pole. It is possibly identi- 
 cal with the celebrated Moses Fork cannel and other cannel deposits 
 in Kentucky. This belt of cannel varies much in width, but it is often 
 2 or 3 miles across, and while the bed is not entirely persistent, it is 
 seldom less than 20 inches thick. It is quite pure and will compare 
 favorably with the celebrated Kanawha cannel, which comes at the same 
 geological horizon. 
 
 On the left branch of Twelve Pole , one-half mile above the mouth of 
 Brush Creek, this cannel coal shows as follows : 
 
 Ft. in. 
 
 Massive sandstone - 
 
 Coal, bituminous 0 10") ^ 
 
 Rock, dark 0 8 4 
 
 Cannel 2 6 j 
 
 On Little Laurel , a branch of Hezekiah Creek (tributary of the left 
 fork of Twelve Pole), the cannel exhibits the following: 
 
 Ft. in. 
 
 Sandstone 
 
 Coal, bituminous 1 O') 
 
 Bone coal 0 8 I in * 
 
 Cannel 3 If 
 
 Bone coal * 1 8j 
 
WHITE.] 
 
 THE UPPER FREEPORT COAL. 
 
 157 
 
 0 
 6 
 
 1 
 3 
 
 7 
 0 
 5 
 5 
 2 
 
 8 
 
 5 
 
 6 J 
 
 Feet. 
 
 27 
 
 On /Saw Pit branch of Cove Creek the following section was meas- 
 ured : 
 
 Ft. in. 
 
 Coal, blossom 2 0 ) 
 
 Sandstone ■- 25 0 S 
 
 Coal 0 
 
 Slate, gray 0 
 
 Coal, bituminous 1 
 
 Cannel 1 
 
 Coal, splint 1 
 
 Slate and slaty coal 0 
 
 Coal 0 
 
 Slate 0 
 
 Coal, splint 0 
 
 Slate, blue 0 
 
 Coal, splint 1 
 
 8 
 
 In Sugar Camp Hollow , a short distance above Jesse Queen’s, the 
 Upper Freeport coal exhibits the following structure: 
 
 Ft. in. 
 
 Sandstone, massive ^ 
 
 Coal 2 4 
 
 Slate 0 2 
 
 Coal, splint « 1 2 
 
 Slate, gray 0 4 
 
 Coal r 0 2 
 
 Slate, gray 0 4 
 
 Coal, splint 0 8 f 
 
 Slate, gray 0 4 
 
 Coal 1 6 
 
 Slate, dark 0 9 
 
 Coal 0 7 
 
 Slate 0 6 
 
 Coal 0 1 J 
 
 Shaly sandstone 15 
 
 Coal 1 
 
 Ft. in. 
 
 8 11 1 
 
 Ft. in. 
 25 5 
 
 6 J 
 
 On Trough Creelc , near James Rainey’s, this coal exhibits the fol- 
 lowing: 
 
 Massive sandstone 
 
 Ft. 
 
 in. 
 
 Cannel slate 
 
 .... 0 
 
 5 
 
 Coal, splinty 
 
 
 9 
 
 Slate 
 
 0 
 
 1 
 
 Coal, splint 
 
 1 
 
 0 „ 
 
 Flaggv sandstone and shale 
 
 
 
 Cannel slate 
 
 0 
 
 8 ' 
 
 Coal 
 
 p. 
 
 1 
 
 Slate 
 
 0 
 
 a 
 
 Coal 
 
 .... 0 10 [ 
 
 Shale, gray 
 
 
 6 1 
 
 Coal 
 
 
 lj 
 
 Ft. in. 
 
 3 S') 
 
 Ft. in. 
 24 7 
 
158 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65 . 
 
 At Greene Porter’s, on tlie right bank of Twelve Pole, the Upper 
 Freeport bed shows the following: 
 
 Ft. in. 
 
 Coal 
 
 . Clay 
 
 Shale and coal 
 
 Coal 
 
 Bony coal and slate 
 Coal 
 
 1 0 4 
 0 5 
 
 0 9 
 
 1 10 | 
 
 1 0 j 
 
 2 4 j 
 
 Ft. in. 
 7 4 
 
 From this point on west to the Kentucky line on the Tug River noth- 
 ing is known of the Upper Freeport coal, and at Warfield it seems to 
 be absent from the section, but this may possibly be due to the fact 
 that its horizon there overtops the summit of the hills. 
 
 In western Pennsylvania there are large areas, especially in Beaver 
 County, where this coal is either absent or else too thin to mine ; so it 
 enters Ohio not as a persistent bed, but occurring in patches, and this 
 characteristic seems to remain with it there, from the Pennsylvania line 
 entirely across the State to the Kentucky border at Ironton. 
 
 Even along the Ohio River from the Pennsylvania line down to where 
 this bed dips below the same, it is generally absent, and Prof. Orton 
 thinks it is still absent in the Steubenville shafts, the coal mined there 
 being the Lower Freeport bed, instead of the Upper Freeport as was 
 formerly supposed. 
 
 In eastern Ohio it is known as bed No. 6 in the Ohio scheme of num- 
 bers, but in other portions of the State, as Prof. Orton has shown, it 
 was often called No. 7. The following list of Ohio names for this bed 
 will indicate regions in that State where the bed becomes prominent: 
 “Big Vein” of Salinesville, “Dell Roy,” “Cambridge,” “Alexander,” 
 “Bayley’s Run,” “ Norris,” “ Happy Hollow,” “Waterloo.” 
 
 Section near Kenova , West Virginia . — After passing beneath the Ohio 
 River above Steubenville, this bed never emerges from the same until 
 within 2 miles of the Kentucky line, and if the Steubenville shaft 
 coal be the Lower Freeport, then the Upper one is absent over a wide 
 region along the Ohio River, for it appears to be absent in several bor- 
 ings, notably at Parkersburg and Pomeroy. It is reported from a boring 
 at Huntington, however, as 10 feet thick, though where it comes up to 
 the level of the Chesapeake and Ohio Railroad at the east end of the 
 Big Sandy bridge, 10 miles below Huntington, the bed is worthless, 
 as shown by the following structure there : 
 
 Ft. 
 
 l 1 Ft. 
 
 3 J, 5 
 
 1 j 
 
 Coal 
 
 Shale 
 
 Coal, slaty 
 
WHITE. J 
 
 THE UPPER FREEPORT COAL. 
 
 159 
 
 Section in RitcMe County , West Virginia. — Where this bed is brought 
 to the surface on the Volcano anticlinal in Ritchie County, West Vir- 
 ginia, it has the following structure, according to Stevenson : 
 
 Ft. in. 
 
 Coal 2 6 ^ Ft. in. 
 
 Sandstone, gray r .. 3 6 6 8 
 
 Coal 0 8 J 
 
 THE UPPER FREEPORT LIMESTONE. 
 
 Below the coal just described, at an interval which varies from 0 to 
 40 feet, there comes a limestone which was named from the same local- 
 ity as the coal. It is quite generally distributed in Pennsylvania, north- 
 ern West Virginia and Ohio, but in the southwestern part of West 
 Virginia it appears to be absent, since it has never been reported from 
 the region along the Big Kanawha and its tributaries, nor from the 
 region between that and the Big Sandy. • 
 
 The limestone is usually of a light gray color on fresh fracture, but 
 some of the layers are always buffish when weathered, owing to in- 
 cluded iron. Frequently the rock presents a brecciated aspect, as if 
 made from the broken fragments of an older limestone. 
 
 Fossils are rare in this bed except a minute univalve which looks as 
 if it might be of fresh water origin. Some layers of this stratum gen- 
 erally contain a considerable amount of carbonate of magnesia, and 
 occasionally enough to constitute it a good rock for the manufacture of 
 hydraulic cement. 
 
 The thickness varies from 1 foot up to 30 feet as a maximum, though 
 the average might be placed at 5 to 8. It makes an excellent lime for 
 fertilizing purposes, and is much sought after to enrich the barren soil 
 lauds above, though it is occasionally mined for use in blast furnaces, 
 as on the Alleghany River between Freeport and Kittanning, where it 
 is unusually thick. 
 
 In Ohio this bed has been given several names, as u Shawnee,” 
 u White,” u Buchtel,” etc. There, also, as in Pennsylvania and West 
 Virginia, it occasionally becomes iron-bearing and some or all of its 
 layers develop into iron ore, which is known in Ohio as the “Buchtel” 
 ore, and in Pennsylvania as the “ Summit” ore. 
 
 THE BOLIVAR FIRE CLAY. 
 
 When the Upper Freeport limestone is absent, or but slightly rep- 
 resented, there occasionally comes into the section at its horizon a bed 
 of excellent fire clay, which from having long been mined near Bolivar, 
 Westmoreland County, Pennsylvania, is generally known as the Bolivar 
 clay. As there developed it shows a fine quality of non-plastic clay 
 which is used in the manufacture of fire brick and gas retorts. Tt also 
 occurs in several other regions of Westmoreland County, as well as in 
 Fayette and other Pennsylvania counties. 
 
160 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65 
 
 This clay has been reported as valuable at only two or three points 
 in Ohio, viz, in Jefferson and Muskingum Counties, while in West Vir- 
 ginia it is known to be valuable in only one region, viz, on Deckers 
 Creek, in Preston and Monongalia Counties. 
 
 THE UPPER FREEPORT SANDSTONE. 
 
 As a rule the main portion of the interval between the Upper and 
 Lower Freeport coals is occupied by sandy shales or thin flaggy layers 
 of sandstone, separated by shales, but occasionally a bed of massive 
 sandstone makes its appearance at this horizon and it has received the 
 name of Upper Freeport Sandstone. It is quite prominent in some por- 
 tions of Pennsylvania, but appears to be generally absent in Ohio. It 
 is also conspicuous along the Great Kanawha and in all the region of 
 West Virginia, southwest from there, sometimes attaining a thickness 
 of 75 feet, while in Pennsylvania it is seldom more than 30 feet. 
 
 When this sandstone is not present as a massive rock there occasion- 
 ally occurs a thin bed of coal in the interval between the Upper and 
 Lower Freeport coals, and I have termed it 
 
 THE MIDDLE FREEPORT COAL. 
 
 This bed is shown in Section 66 at the typical Freeport locality, and 
 as already stated in connection therewith, its presence in other sections 
 may have led to some confusion in identifications. It is not a regular 
 member of the series, however, and is probably never much thicker than 
 at Freeport, viz, 2 feet. 
 
 The interval between the Upper and Lower Freeport coals varies 
 greatly in thickness, running up sometimes to 80 and again thinning 
 away tq 20- odd feet, as shown in Section 65. 
 
 THE LOWER FREEPORT COAL. 
 
 This bed is quite as variable, or even more so than the Upper Free- 
 port above. The rule is that whenever one of these beds has a fair 
 development the other is poor or worthless, but in addition to this un- 
 certainty, they are both frequently thin, or practically absent from the 
 section at the same time, so that no one should look upon any of these 
 coal beds as being continuously valuable over wide areas. 
 
 As shown in Section 66 at the type locality of this bed, it is even 
 more complex in its structure than the Upper Freeport above, being 
 split into two well defined layers separated by a stratum of clay and 
 limestone. It is quite probable that this dividing layer may at times 
 thicken up greatly as all other rocks do, and separate the two layers of 
 coal by an interval of several fret, thus making two apparently distinct 
 coal beds, but which should really be classed as members of one. 
 
 If Messrs. Chance and Platt are correct in the identifications of the 
 Lower Freeport coal in Jefferson and Clearfield, there are large areas 
 in both of these counties where this coal is quite valuable, since it is 4 
 
THE LOWER FREEPORT COAL. 
 
 WHITE.] 
 
 161 
 
 to 7 feet thick and of excellent quality, though it is always separated 
 into two or three benches by partings of slate. 
 
 The upper portion of the Lower Freeport bed often has a tendency 
 to become cannelly, as at Freeport, and some highly bituminous shale 
 is frequently present at this horizon, even when the coal is absent. 
 
 Another very fine development of the Lower Freeport coal is in the 
 vicinity of Fairmont, Clarion County, Pennsylvania, where according to 
 Chance it is 5 to 7 feet thick without any partings, and furnishes ao 
 excellent quality of gas coal, as it does in the Reynoldsville region of 
 Jefferson County. 
 
 In Ohio the reputation of the coal as a patchy deposit is fully sus- 
 tained, since Prof. Orton says of it (Yol. Y, p. 16G, Ohio Geological 
 Survey), “this is a seam the horizon of which can be followed through- 
 out the entire field, but which becomes workable at comparatively few 
 points.” 
 
 In eastern Ohio it is called No. 5, but in Stark County and southwest- 
 ward it is known as No. 6a, while the synonyms, “ Whan” ‘‘Steuben- 
 ville Shaft,” “Roger,” “Hamden Furnace,” and “Hatcher” indicate 
 localities where the bed becomes important. 
 
 If the “ Steubenville Shaft” bed really represents this coal instead of 
 the Upper Freeport, then there is quite a large field of it along the Ohio 
 River, for it is found of good thickness in every boring as far south as 
 Moundsville, West Yirginia, where it underlies the Ohio by more than 
 600 feet. 
 
 Section near Philippi , Barbour County , West Virginia . — In Preston, 
 Monongalia, Mineral, and Tucker Counties, West Yirginia, this bed is 
 quite thin and often absent entirely, so it is not mined till- we go south 
 into Barbour County, where it thickens up and in the vicinity of Phil- 
 ippi exhibits the following structure : 
 
 Coal 
 
 Slate 
 
 Coal 
 
 Slate and coal 
 Coal 
 
 Ft. in. 
 
 1 10 A 
 
 0 8 Ft. in. 
 
 0 6 \ 5 10 
 
 0 10 | 
 
 2 0 J 
 
 Nothing is known of the Lower Freeport from Philippi on southwest- 
 ward along the eastern margin of the Appalachian field until the Great 
 Kanawha River is reached, except in the Roaring Creek field, where it 
 is only 2 feet thick and 25 feet below the upper bed. 
 
 But from the fact that this coal becomes one of the principal beds in 
 the Kanawha region, and from there on southwestward into Kentucky, 
 it is inferred that it is also a valuable bed at some points between Phil- 
 ippi and the Big Kanawha. 
 
 On this latter stream the Lower Freeport appears to be the parent of 
 two valuable beds known respectively as the Coalburg and Winnifrede 
 veins. The former certainly belongs to this horizon, and the latter 
 
 Bull. 65 U 
 
162 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 f BULL. 65. 
 
 probably does, though formerly I was inclined to refer it to the horizon 
 of the Upper Kittanning. The Lower Coal Measures thicken up so 
 greatly in that region, however, and the intervals separating the Coal- 
 burg and Winifrede beds from the top of the series and from each other 
 vary so much that it seems more probable they are both members of 
 the complex Lower Freeport coal. The Coalburg and Winifrede beds 
 are themselves complex, being always separated into two or three 
 benches by layers of very hard slate or bony coal locally known as 
 “nigger head.’ 7 They usually furnish the variety of coal known as 
 “splint,” and the Kanawha “splint” is highly prized as a general do- 
 mestic fuel. These two beds are quite irregular in their thickness and 
 one or both are often too thin to mine, but they appear to be much more 
 regular and persistent southwest from the Kanawha than the Upper 
 Freeport, since they furnish valuable coal clear across to the Big Sandy 
 Biver, the celebrated Peach Orchard coal of Kentucky coming at the 
 horizon of either the Coalburg or Winifrede bed, or both combined. 
 This latter view is the more probable, since at the tunnel near the New 
 Peach Orchard mine the coal is seen splitting up till it is scattered 
 through more than 40 feet of rock material. 
 
 Section of bed at Coalburg , Kanawha County , West Virginia. — The 
 following section shows the variations in the structure of the Coalburg 
 bed at its typical locality : 
 
 Splint coal 
 
 “Nigger head” 
 
 Splint coal 
 
 Shale 
 
 Soft coal 
 
 6 in. to 10 ft. 
 4 in. to 8 in. 
 2 \ ft. to 3* ft. 
 1 ft. to 8 ft. 
 1 ft. to H ft. 
 
 Section at Winifrede, Kanawha County , West Virginia. — The struc- 
 ture of the Winifrede coal at Winifrede is as follows: 
 
 Ft. in. 
 
 Gray splint 0 5 
 
 Soft coal 0 5 
 
 Gray splint 0 3 
 
 Soft coal 0 3 
 
 Gray splint 1 2 
 
 Soft coal 1 3 
 
 Slate 0 5 
 
 Soft coal 1 8 
 
 | Ft. in. 
 I 4 10 
 
 I do not know of any locality in the Kanawha Yalley where both the 
 Winifrede and Coalburg beds are mined one above the other in the 
 same hill, for when one is good the other happens to be worthless, and 
 this is so constantly true that, were it not for the fact that the Coal- 
 burg bed is only 100 feet below the Kanawha black flint while the Win- 
 ifrede seam is 175 to 200 feet below the same datum line, I would be 
 strongly inclined to believe that they were one and the same coal. 
 
 Section at mouth of Blaine Creelc, Lawrence County , Kentucky . — In de- 
 scending the Big Saudy Biver the Lower Freeport sinks below water 
 
VTOITB.] 
 
 THE LOWER FREEPORT LIMESTONE. 
 
 163 
 
 level at the mouth of Blaine Creek, 6 miles below Louisa, where it ex- 
 hibits the following structure : 
 
 Ft. in. 
 
 Massive sandstone . 
 
 Coal 
 
 Fire clay 
 
 Sandy shale 
 
 Coal 
 
 Shale with iron ore 
 
 Coal, slaty 
 
 Shale, blue 
 
 Coal 
 
 . 0 10 | Ft - 
 .5 0 > 7 
 
 .2 0 j 
 . 0 10 ) 
 
 .1 0 [ 
 
 . 1 0 }> 5 
 
 1 q ! 
 
 in. 
 
 10 
 
 7 
 
 TILE LOWER FREEPORT LIMESTONE. 
 
 The conditions preceding the spread of a great coal marsh seem to 
 have been eminently fitted for the production of limestone deposits, 
 especially in the Pennsylvania and Ohio regions, for, with few excep- 
 tions, a limestone is found close under every coal bed, and this is true 
 of the Lower Freeport horizon. This limestone very much resembles 
 the one under the Upper Freeport coal, except that it is usually thinner 
 and more earthy. It also contains the same univalve fossil, and no 
 others, so far as the writer is aware, thus showing that it too is a fresh- 
 water deposit. It contains a considerable quantity of carbonate of 
 magnesia and occasionally, as at the locality of Section 103, furnishes 
 material for the manufacture of hydraulic cement. 
 
 Considerable iron ore is also found at this horizon, and the limestone 
 is generally of a buffish cast from the disseminated iron. From this 
 fact it and the Upper Freeport limestone above are generally called the 
 “buff” limestones in southern Ohio. 
 
 In West Virginia this limestone has not been recognized anywhere 
 in the northern part of the State, and it is certainly absent entirely 
 along the Great Kanawha. An impure limestone is sometimes found 
 in connection with the Peach Orchard coal of Kentucky, which is pos- 
 sibly identical with the Lower Freeport. 
 
 THE LOWER FREEPORT SANDSTONE. 
 
 The next lower stratum that has a general distribution over the Appa- 
 lachian field is known as the Lower Freeport sandstone. Section 66 
 shows the thickness and structure of this sandstone at its typical 
 locality, and there it is seen to be double, with a coal embedded in its 
 lower portion, the whole being 62 feet thick. That the 15 feet of sand- 
 stone under the coal at Freeport belongs properly with the main sand- 
 stone above is known from the fact that at one locality the coal is seen 
 disappearing entirely and then the two beds of sandstone unite into 
 one solid mass. 
 
 This rock is always of a grayish white color, generally quite hard 
 often containing pebbles as well as much feldspar, which decomposing 
 permits the rock to disintegrate readily and weather into fantastic 
 
164 
 
 THE NORTHERN BITUMINOUS COAL FIELD! 
 
 [BULL. 65. 
 
 shapes. It is more persistent as a massive rock than the Mahoning 
 even, but unlike the latter it is seldom used for building purposes. 
 This is owing to its hardness, coupled with the fact that it will not 
 stand the weather well, and also it is often so gnarly and twisted in its 
 bedding that it will not split evenly. 
 
 This sandstone is never less than 30 feet thick in the Pennsylvania 
 region, and it frequently rises to 75 and even 100 feet in some localities, 
 making a bold cliff or bluff wherever its outcrop is above drainage, and 
 thus becoming a conspicuous feature in the topography of the Lower 
 Coal Measures. 
 
 Throughout a large portion of Beaver County, Pennsylvania, this 
 sandstone is 75 to 80 feet thick, and near its center is a very hard 
 calcareo- siliceous layer 2 or 3 feet thick, which may possibly represent 
 the Johnstown Cement limestone in other portions of the State. 
 
 The sandstone maintains about the same thickness throughout east- 
 ern Ohio as in Beaver County, and continues on around to southern 
 Ohio with a thickness of 30 to 50 feet. 
 
 It enters West Virginia from Pennsylvania as a very massive bed, 
 50 to 75 feet thick in Monongalia and Preston Counties, while in 
 Tucker, Taylor, Barbour, and Bandolph, it is still thicker and more 
 pebbly even than the Pottsville conglomerate. South westward through 
 Bandolph, Webster, Braxton, and Clay, this sandstone keeps on increas- 
 ing in thickness, and when the Big Kanawha is reached it has swelled 
 out in a wonderful manner, becoming 250 to 300 feet thick, and remain- 
 ing the same across to the Big Sandy, often crowning the hills and 
 ridges with cliffs weathered into turreted and chimney-shaped forms. 
 When attaining this immense thickness it often consists of three or four 
 sandstones, with shales and two or three coal beds in ter stratified. 
 
 This rock has produced a small quantity of oil at Fairview, Marion 
 County, West Virginia, and is generally known as the “gas sand,” in 
 the drillers 7 parlance, since it often produces considerable quantities of 
 natural gas. 
 
 THE UPPER KITTANNING COAL. 
 
 Throughout several counties of Pennsylvania a third bed of good 
 coal occurs at 80 to 120 feet below the top of the series, and to this 
 Messrs. Chance, Platt, and other Pennsylvania geologists, have given 
 the name Upper Kittanning, though the bed in question is not work- 
 able at Kittanning or anywhere near that town, as may be seen from 
 Sections 60-66 along the Alleghany Biver, since it is thin and unim- 
 portant in that region. The Messrs. Platt at one time identified this 
 coal with the Lower Freeport bed in Cambria, Clearfield, and Jefferson 
 Counties, calling the coal which is now termed Lower Freeport there 
 the Middle Freeport, and it is barely possible that this first arrange- 
 ment of the stratigrapliical order was the correct one in many regions, 
 since, as already shown (see 66), there is a Middle Freeport coal even 
 
WHITE. J 
 
 THE UPPER KITTANNING COAL. 
 
 165 . 
 
 at Freeport, and in addition the Lower Freeport bed is itself so com- 
 plex that either half of it might at any time separate from the other 
 and both become independent beds. 
 
 But however the questions suggested may turn out, the fact remains 
 that at many localities in Pennsylvania, at least, there are three dis- 
 tinct coal beds between the Ferriferous limestone and the Lower Free- 
 port coal, as shown in Sections 64, 65, and 66. 
 
 Westward in Ohio, however, the Upper Kittanning coal appears to 
 be either wanting entirely in most cases or else coalesced with the 
 Middle Kittanning bed, since Prof. Orton finds no place for it as a reg- 
 ular member of the Ohio series, but puts it down as a synonym for the 
 Lower Freeport seam. (See Yol. V, p. 126, Ohio Survey.) 
 
 In West Virginia the Upper Kittanuing bed first appears in the sec- 
 tions along the Tygart’s Valley River (96 and 97), where it is 2 to 3J 
 feet thick, and a rather fair coal ; but it appears to be absent entirely 
 in the Newburg shaft, Preston County, unless it is combined with the 
 Middle Kittanning there, while in the Korth Potomac basin near Davis 
 it is represented by a mere streak. In the Kanawha field two or three 
 thin beds come at this horizon, and one of them is frequently cannel, 
 and the same horizon can be recognized on the Guyandotte River, in 
 Wyomiug County (Section 117). 
 
 Chance says that it is the main cannel horizon in Pennsylvania, the 
 Kew Bethlehem, Korth Washington, and Murrinsville cannel deposits 
 coming at this horizon. If the Darlington cannel, of Beaver County, 
 comes at this same horizon, then the iuterval separating the Upper 
 and Middle Kittanning beds has there thinned entirely away, and thus 
 brought the two into direct contact. This might well be, since the Dar- 
 lington cannel rests directly on 2 feefeof bituminous coal, below which, 
 through a shale interval of 30 feet, comes the undoubted Lower Kit- 
 tanning coal, underlaid by its great bed of fire clay. This would account 
 for the absence of the coal in Ohio, if it really does unite with the Mid- 
 dle Kittanuing before crossing the Pennsylvania-Oliio line. 
 
 This bed appears to attain its greatest importance in Pennsylvania, 
 along the eastern border of the coal field through the counties of Jef- 
 ferson, Clearfield, Cambria, and Somerset, where it has been fully de- 
 scribed by Messrs. Platt and Chance. The general sections already 
 given show the horizon and structure of this bed at numerous points, 
 so that no further description of it is necessary. 
 
 THE JOHNSTOWN (CEMENT) LIMESTONE. 
 
 Lying only 2 to 5 feet below the coal just described, there occurs, Over 
 a wide region in Pennsylvania, a bed of magnesian limestone, which Mr. 
 Franklin Platt named the Johnstown Cement, from its occurrence at the 
 city of Johnstown, Cambria County. It is almost an exact counter- 
 part of the Lower Freeport limestone of the counties farther west in 
 physical aspect, chemical composition, fossils, and everything else, and 
 
166 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65 . 
 
 this is one of the facts which, taken in connection with the entire ab- 
 sence of this limestone in the western tier of counties and in Ohio, has 
 sometimes led to the suspicion that possibly the Johnstown Cement 
 and the Lower Freeport limestone of Butler and Beaver Counties are 
 identical. Still there are other facts of stratigraphy which appear to 
 forbid such an hypothesis, and hence, until it can be shown otherwise 
 by more positive demonstration, we must accept the strati graphical 
 horizon given the Johnstown Cement first by Messrs. Platt, whose 
 labors moved it up from the horizon of the Ferriferous limestone, to 
 which the First Geological Survey of Pennsylvania had erroneously 
 assigned it. The stratum ranges in thickness from 1 to 8 feet, and 
 when it is 5 feet or more some of the layers often make good lime for 
 agricultural or other purposes ; but when the bed is only 1 to 3 feet 
 thick it is usually too impure to slake well. This stratum has not been 
 recognized at any point within West Virginia with which the writer is 
 familiar, and it thus appears to be generally absent from the series in 
 that State. 
 
 THE MIDDLE KITTANNING COAL. 
 
 Whatever uncertainty may exist concerning the exact horizon of the 
 coal which has just been described under the name of Upper Kittan- 
 ning, there is none with reference to the next lower bed, for it is such 
 a constant member of the series that its relations to the other rocks are 
 seen in nearly every section. This bed was formerly called the Upper 
 Kittanning, until Messrs. Platt and Chance discovered that the coal 
 last described was a member of the Kittanning group, and then the 
 coal in question was lowered to the name of Middle Kittanning. 
 
 In the vicinity of Kittauning (Section 63), and along the Alleghany 
 Piver below (Sections 64, 65, and 66), this bed is thin and unimportant, 
 but west from this it thickens up and is the most important seam in 
 Butler, Lawrence, and Beaver Counties, the coal being quite pure and 
 highly esteemed for gas, steam, and domestic purposes, though it sel- 
 dom exceeds 4 feet in thickness, and is often much less. This is the 
 famous “ Clin ton,” “Rock Point,” and “Hog Hollow ” coal along the 
 Beaver River. It is always divided by one or more thin slate partings, 
 one of which is usually near the bottom. 
 
 Eastward from Butler County, through Armstrong, Clarion, Jeffer- 
 son, and Clearfield, this bed, according to Platt and Chance, declines 
 much in thickness and value, so that it is seldom mined, except occa- 
 sionally for domestic purposes. 
 
 Still farther eastward, however, in the Broad Top coal field of Hunt- 
 ingdon and Bedford Counties, it thickens up and is apparently repre- 
 sented by the “Barnet” coal of that region. 
 
 Southward from Pennsylvania, in Maryland and northern West 
 Virginia, this coal is sometimes thick enough to mine, though seldom 
 exceeding 2J to 3 feet. At the southern end of the Korth Potomac 
 
WHITE.] 
 
 THE MIDDLE KITTANNING COAL. 
 
 167 
 
 coal basin it practically unites with the Lower Kittanning below, and 
 is mined with the latter where that bed is opened near Thomas ; but at 
 the Davis mine, further south, the parting slates have thickened up to 
 20 feet and separated it from the Lower Kittanning again. 
 
 Section at Neioburg , Preston County , West Virginia . — In the deep 
 shaft at Newburg, Preston County, West Virginia, this coal has the 
 following structure and relations to other beds : 
 
 1. Lower Freeport sandstone 
 
 Ft. In. 
 
 rCoal 1 oS 
 
 o r. I AT- -Ml tr-i Slate 0 3 Ft. in. 
 
 2. Coal, Middle Kit- ^ Coal dat 8 0 7 3 
 
 tannin S | Clay 2 Ol 
 
 fCoal, good 2 0 j 
 
 3. Fireclay and stales - 15 0 
 
 4. Coal, Lower Kittanning, with several partings 9 5 
 
 Here it is possible that both the Upper and Middle Kittanning beds 
 are represented in No. 2, and they are only 15 feet above the Lower 
 Kittanning coal. 
 
 In the Great Kanawha field, this bed, although only 3 to 4 feet thick, 
 is very pure and valuable, being known there under the names of “Ce- 
 dar Grove,” “Trimble,” “Arno,” and others. 
 
 In the Wyoming County section (117) two beds are often found at 
 this horizon, separated by 20 feet of shales, but the lower one appears 
 to be the main coal. The same thing is seen in the Peach Orchard 
 section (119), where the lower one is a “splint” coal, thin, but of excel- 
 lent quality. 
 
 In Ohio this coal becomes the most important bed of all the coals in 
 that State, according to Prof. Orton, since it is almost constantly work- 
 able from where it enters Columbiana County on the east to where it 
 leaves the State near Ironton at the southwest. The numerous names 
 it has received in Ohio will serve to illustrate its importance in the 
 mining industry there, of which the following is a partial list: “ No. 4, 
 in Ohio and Yellow Creek Valleys at the east; “ No. 6,” in Stark County 
 and southwestward; “ Hammondsville Strip Vein,” “ Onasburg,” “ Pike 
 Run,” “Dennison,” “Coshocton,” “Upper Zanesville,” “Upper New 
 Lexington,” “ Nelsonville,” “ Straitsville,” “Great Vein” of the Hock- 
 ing Valley, “ Carbondale,” “Mineral City,” “Upper Zaleski,” “Wash- 
 ington Furnace,” “ Sheridan,” etc. 
 
 The tracing of this bed through Ohio, and its identification at many 
 points where it had formerly been confused with other beds, is due 
 largely to the labors of Prof. Orton, the present efficient director of the 
 Ohio Geological Survey. The structure of the coal where it attains a 
 considerable thickness, as in the Hocking Valley, is always quite com- 
 plex, there being several parting slates, as may be seen from Sections 
 105 and 10G. 
 
168 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65 . 
 
 Section in Hoclcing Valley, Ohio . — The following, from Yol. Y, Ohio 
 Geology, will serve to illustrate the general structure of this bed when 
 at its maximum development: 
 
 Ft. in. 
 
 Top coal ...2 7 ' 
 
 Soft coal, rejected 0 4 
 
 Coal 4 2 
 
 Bone coal, rejected 0 6 [ 
 
 Second slate * 0 2 1 
 
 Coal 1 6 
 
 First slate 0 1 
 
 Coal 2 4 J 
 
 Ft. in. 
 11 ? 
 
 Section at Neic Straitsville, Perry County . — The following is the struc- 
 ture at New Straitsville, p. 954, loc. cit.: 
 
 Coal 
 
 Bone coal 
 
 Coal 
 
 Soft coal. 
 
 Slate 
 
 Coal 
 
 Slate 
 
 Coal 
 
 Ft. in. 
 
 1 2 ' 
 0 2 
 4 0 
 
 u o 
 
 2 1 
 
 0 1 
 
 1 11 . 
 
 Ft. 
 
 10 
 
 According to Orton this bed changes in character from a good coking 
 coal in eastern Ohio to an open-burning one from New Lexington south- 
 westward. The reader will find the coal fully described in Yol. Y, Ohio 
 Geology. 
 
 The interval separating the Middle Kittanning coal from the Lower 
 Kittanning bed varies greatly both in thickness and composition in the 
 different regions of the Appalachian field. In western Pennsylvania 
 and eastern Ohio the interval is usually only 20 to 30 feet and generally 
 occupied with dark slates or shales holding iron nodules, and it seldom 
 surpasses 40 feet anywhere in Pennsylvania, while in northern West 
 Yirginia it locally thins away to an insignificant parting, but to the 
 south westward in the Great Kanawha region, and from there across to 
 the Big Sandy, it often swells up to 100 feet and occasionally attains a 
 thickness of 165 feet (Section 115), with some massive sandstone at 
 several horizons. In southwestern Ohio a massive sandstone 30 to 40 
 feet thick often occupies the interval to the exclusion of shales. 
 
 In the Great Kanawha region a siliceous limestone makes its appear- 
 ance in this interval and seems to have quite a wide distribution in that 
 region and southwestward to the Big Sandy. It is well exposed near 
 the mouth of Campbell’s Creek, and I have designated it the Campbell’s 
 Creek limestone from that locality. This stratum seems to be present 
 even in northern West Yirginia, since in Sections 95 and 96, at Moats- 
 vi lie and Yalley Falls, respectively, a bed of siliceous limestone occurs 
 20 feet above the Lower Kittanning coal. 
 
 Along the Tug Fork of Big Sandy there are siliceous limestones at 
 
 
 
WHITE.] 
 
 THE LOWER KITTANNING COAL. 
 
 169 
 
 several horizons above the Campbell’s Creek bed, as shown in Section 
 119, there being two and sometimes three within the horizon of the 
 Lower Freeport sandstone, so that these must not be confounded with 
 the one in question. 
 
 The bottom layers of this shale interval immediately above the Lower 
 Kittanning coal are nearly always filled with fossil plants. They occur 
 in great variety and abundance wherever the rock material in the roof 
 of the underlying coal is a shale, and this is the horizon par excellence 
 for the collector of plants from the Lower Coal Measures. 
 
 These beds have been thoroughly explored at only one locality in the 
 Appalachian field, viz, Cannelton, Beaver County, Pennsylvania, where 
 Mr. I. F. Mansfield has collected systematically for Prof. Lesquereux 
 during several years, the results of which are recorded in Report P, 
 Yols. I and II, Second Geological Survey of Pennsylvania. The list 
 includes a large number of species, several of which are peculiar to 
 that locality. 
 
 THE LOWER KITTANNING COAL. 
 
 The next lower bed of this series, though formerly named simply 
 the Kittanning coal by Rogers, is now called the Lower Kittanning. 
 Although seldom attaining any unusual thickness, it is probably the 
 most persistent bed in the entire Appalachian field, and has a workable 
 thickness over a larger area than any other. In Pennsylvania it fur- 
 nishes from 3 to 4 feet of valuable fuel over large areas in every county 
 where its outcrop is due. Of course, like all other coals, it thins down 
 locally and becomes worthless over considerable areas, but the barren 
 patches on the horizon of the Lower Kittanning bed are fewer and 
 smaller than those at the horizon of any other coal in the entire Lower 
 Coal Measures. If the Middle Kittanning is the more important coal 
 in Ohio, the Lower surpasses it in Pennsylvania and West Virginia, 
 so that the difference in favor of the former in Ohio is much more 
 than offset in the latter two States. This coal is also a composite seam, 
 and when it acquires considerable thickness is often split into several 
 divisions by separating slates. In the Pennsylvania field these slates 
 are usually mere knife edges, and add but little to the total thickness 
 of the bed, except in the eastern portion of the field, where in Clear- 
 field, Bedford, and Huntingdon it often has a layer of impure fire clay 
 or gray shale separating the bottom member from the middle one. 
 
 The u Fulton vein ” of the Broad Top field appears to be identical 
 with this coal, though the writer was formerly inclined to regard it as 
 identical with the Clarion (see T 3 , Second Geological Survey of Penn- 
 sylvania), and bed “A” of the Tipton Run series is probably the same. 
 
 The u Bloss vein” of Tioga County seems to be referable to this same 
 horizon both with reference to structure and its position in the column 
 of rocks (Sections 50 and 51). 
 
 In the Georges Creek field of Maryland this is often known as the 
 u 6-foot” bed, and its structure there is given in Section 92. From Elk 
 
170 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Garden southward along the North Potomac to where this bed passes 
 under draiuage level, near Gorman, it is so badly split up with slate as 
 to be rather valueless, but where it emerges to daylight again on the 
 other side of the Cheat-Potomac divide, near Thomas, it has become a 
 splendid vein nearly 11 feet thick, as shown in Section 94, from which 
 0 feet of excellent coal is miued without taking out the bottom member. 
 As already stated, the bed attains its great thickness in this region by 
 the thinning away of the shales which usually separate the Middle and 
 Lower Kittanning beds, thus permitting the two practically to unite 
 into one. The coal from it here is prized for smithing purposes quite 
 as highly as the celebrated Blossburg bed, with which it appears to be 
 identical. It has also been successfully coked in this Tucker County 
 field, since it is nearly always a good coking coal everywhere. 
 
 Section at Newburg, Preston County, West Virginia . — In the deep shaft 
 at Newburg, Preston County, West Virginia, the Lower Kittanning has 
 the following structure: 
 
 Ft. in. 
 
 Coal 
 
 Shale, gray 
 
 Coal 
 
 Bony coal . . 
 
 Coal 
 
 Black slate 
 Coal 
 
 0 10 ^ 
 
 0 10 
 
 o 6 J Ft. in. 
 0 3 > 9 & 
 4 6 ’ 
 
 0 6 
 2 0 
 
 Sections 95 and 96 show the structure of this bed where it is brought 
 to the surface by the Chestnut Bidge anticlinal, on the Tygart’s Valley 
 Kiver, below Grafton, West Virginia, and, as will be seen, it is there 
 about 5 feet thick. 
 
 On the Great Kanawha Biver, above Charleston, this is one of the 
 principal coal beds, and has long been known there as the CampbelPs 
 Creek vein. At this locality on CampbelPs Creek the coal is 4 to 6 feet 
 thick with only two parting slates, but in passing southward up the 
 Kanawha new partings come in and the old ones thicken up until the 
 bed, with its included rock partings, swells out to a thickness of nearly 
 50 feet, and two of the members are mined independently, the upper 
 one being known as the Peerless bed and the lower one as the Blacks- 
 burg. The upper member never exceeds 3 feet, and is usually about 
 20 feet above the Blacksburg member, which is often 4 to 5 feet thick 
 and is the “ Coal Valley gas vein.” On the Mount Carbon property, 25 
 miles south from CampbelPs Creek, the 20 feet of shales which usually 
 separate the Peerless and Blacksburg members of the Lower Kittan- 
 ning coal thin away to a few inches locally, and both are taken out of 
 the same drift. This is also the condition of affairs at the famous 
 Austead mines of the Hawk’s Nest Coal Company on top of Gauley 
 Mountain. At the head of Cabin Creek, a tributary from the south 
 bank of the Big Kanawha, the Peerless and upper half of the Blacks- 
 burg member couie completely together, forming a bed of excellent gas 
 coal 5£ feet thick. 
 
WHITE.] 
 
 THE KITTANNING FIRE CLAY. 
 
 171 
 
 In Wyoming County, West Virginia, this coal, which is locally called 
 the “ Cook vein,” has a good development, the whole seam with its part- 
 ing slates being about 25 feet thick, as may be seen from Section 117, 
 but the main portion of the bed is about 7 to 8 feet thick, separated into 
 three layers by slate partings of 4 to 6 inches thick. 
 
 This coal rises above the level of the Tug Fork of Big Sandy about 3 
 miles below Warfield and 30 above Louisa. It has been mined to some 
 extent for local use at Warfield, and is known in that region as the 
 “ Warfield coal.” Its structure there is given by Section 119. Above 
 Warfield it dips down under the stream and does not come up again for 
 about 10 miles, or some distance above the mouth of Pigeon Creek, but 
 from there on up Tug Biver it is constantly accessible for about 40 
 miles, until the southward rise of the rocks throws the coal above the 
 tops of the hills near the mouth of Ben Creek, 95 miles above the mouth 
 of Tug. Along this line the coal is seldom less than 3 feet thick and 
 frequently 4 to 5 feet, with only one slate parting 3 to 5 inches thick. At 
 the mouth of Lick Creek and 60 miles from Louisa this coal is 100 feet 
 above the river, and reported 6 to 7 feet thick, with only one thin slate 
 near the center. 
 
 In Ohio the Lower Kittanning coal is almost as persistent as in Penn- 
 sylvania, rarely being absent entirely from the section, and generally 
 having a thickness of 3 feet, with a maximum of 5. 
 
 In the deep oil-borings across southwest Pennsylvania and northern 
 West Virginia this coal is quite persistent, being frequently reported at 
 a depth of 1,500 to 1,800 feet beneath the surface. 
 
 Trie following list of names has been given it in Ohio : Coal No. 3 in 
 Ohio Valley and along Yellow Creek, No. 4 at Leetonia, No. 5 in Stark 
 County and south westward ; also “ Creek vein,” “ Potter’s vein,” “ Lee- 
 tonia,” “ Mineral Point,” “Lower New Lexington,” “Newcastle,” etc. 
 This coal is often neglected in Ohio even when it has a thickness of 2J 
 to 3 feet, because of the great development of the Middle Kittanning 
 coal only a few feet above. Both of these beds have now, through the 
 labors of Newberry, Orton, Boy, and others, been traced from the Penn- 
 sylvania line clear across Ohio to where they pass into Kentucky at 
 Ironton, and have been so well described by Orton in Vol. V, Ohio 
 Geology, that it is unnecessary for the writer to dwell on them longer. 
 
 THE KITTANNING FIRE CLAY. 
 
 Lying directly under the last described coai there comes in many 
 regions a great bed of splendid fire clay which often overshadows the 
 coal in value, since many millions of dollars are invested in manufac- 
 turing the several lines of articles which can be made from this clay. 
 The bed has been named from Kittanning, where it is mined, and here 
 as well as at many localities in Ohio the clay does not all immediately 
 underlie the coal, but some of it is found a few feet lower and nearly 
 on top of the Ferriferous limestone. 
 
172 THE NORTHERN BITUMINOUS COAL FIELD. {bull. 65 . 
 
 Eastward from the Alleghany River this clay does not appear to be 
 very important, bat westward from that point it is generally present, 
 and attains its maximum development along the Beaver, and westward 
 from there down the Ohio; the famous potteries at New Brighton, Roch- 
 ester, East Liverpool, New Cumberland, and other points in these val- 
 leys all deriving their clay from this horizon. 
 
 In the Beaver County region the thickness is generally about 8 to 10 
 feet, but occasionally runs up to 15 and down to 5. It often consists of 
 two portions, an upper “ soft” clay and a lower “hard” clay, the latter 
 being used in the manufacture of fire brick, etc. In western Pennsyl- 
 vania and eastern Ohio this clay bed is often a very valuable element 
 in settling questions of stratigraphy which would otherwise be extremely 
 difficult of solution ; in fact it is valuable for this purpose clear across 
 the Ohio coal field, since, according to Orton, although not entirely per- 
 sistent, yet it furnishes valuable clay mines in every county of its out- 
 crop from the Pennsylvania line across to the Kentucky border. 
 
 In West Virginia (except along the Upper Ohio River) the deposit is 
 seldom of value, being too siliceous, and it has been developed in only one 
 region, viz, near the locality of Section 97, at Ruzuuds, on the Tygartfs 
 Valley River. Here along the crown of the Chestnut Ridge anticlinal 
 the coal above locally disappears, and then a valuable bed of hard clay 
 replaces it, but when the coal comes in again the clay disappears, just 
 as it often does in Ohio, when the hard flinty clay is present. The 
 Glade Fire Brick Works at Kuzums manufacture a good fire brick from 
 this bed. 
 
 THE KITTANNING SANDSTONE. 
 
 The interval between the Lower Kittanning coal and the Ferriferous 
 limestone varies greatly in thickness, sometimes only the clay bed just 
 described intervening, and again the interval thickens up to 50 to 75 
 feet or even more. Whenever the interval attains anything like these 
 last figures we generally find a massive sandstone between the coal and 
 the limestone, and to this has been given the name Kittanning. It 
 sometimes, as on Buffalo Creek, Butler County, Pennsylvania, develops 
 into a great cliff rock of massive and even pebbly sandstone, cutting out 
 the'underlying limestone (Ferriferous). It often furnishes good quarry 
 stone, and a rock occupying this horizon in the series has been quarried 
 and used in building the Government lock and dam near Coal Valley, 
 on the Great Kanawha River. In this region the interval between the 
 Lower Kittanning coal and the Ferriferous limestone thickens up to 150 
 feet, and a local bed of coal, the Brownstown, comes into the series 
 about half way in the interval. In Wyoming County and westward 
 from there the Kittanning sandstone thickens to 100 feet, as seen in 
 Section 117. 
 
 THE BUHRSTONE IRON ORE. 
 
 Resting immediately on top of the Ferriferous limestone there occurs 
 over a very wide area a deposit of iron ore. In Pennsylvania it is often 
 
WHITE.] 
 
 THE FERRIFEROUS LIMESTONE. 
 
 173 
 
 underlaid with cherty material, and hence long ago received the name 
 of “Buhrstone ore,” but it is there also called Ferriferous ore. In Ohio 
 it has a wide distribution and is known under several names, among 
 which are “ Baird” ore, “ Gray” ore, u Limestone” ore. 
 
 The ore generally lies in immediate contact with the limestone, in a 
 slab-like sheet one-half to 1 foot thick, but occasionally, as in Lawrence 
 County, Pennsylvania, on the Houck farm, it locally thickens up to 20 
 feet, entirely replacing the underlying limestone, while again it is absent 
 over wide areas, or represented by nodules scattered through the over- 
 lying shales. When the Ferriferous limestone is absent, its place in 
 the series can often be correctly assigned from the existence of this ore, 
 as is the case in Section 97, at Nuzum’s Mills, West Virginia. This bed 
 was formerly the main ore from which the charcoal furnaces of western 
 Pennsylvania drew their supplies, and it is still the main feeder for these 
 furnaces in southern Ohio. In northern West Virginia some iron ore 
 occurs at this horizon in Monongalia and Preston Counties, and a few 
 inches of it may be seen near the coke ovens on Glady Fork, below 
 Thomas, Tucker County, but in the Great Kanawha region and south- 
 ward toward the Big Sandy it appears to be completely absent as a 
 distinct stratum, though nodules of iron sometimes come at this horizon. 
 
 THE FERRIFEROUS LIMESTONE. 
 
 The occurrence of the iron ore just described resting upon a bed of 
 limestone over a wide area suggested the name 4 ‘Ferriferous” which 
 the early geologists applied to the limestone as well as the ore. 
 
 Tins is the most important and widely distributed limestone of the 
 entire Coal Measure column, important both in an economic sense and 
 as a strati graphical horizon which with ordinary care can be unfailingly 
 recognized by geologists as well as anyone else interested in determin- 
 ing the correct order of the rocks. It differs from the other limestones 
 that we have had so far in the Lower Coal Measures, in being a genuine 
 marine deposit, abounding in fossil criuoids, corals, brachiopods, la- 
 mellibranchs, univalves, etc., a list of the more common forms of which 
 is given on pages 46 and 47, Report QQ, Second Geological Survey of 
 Pennsylvania. 
 
 In Pennsylvania this limestone is confined to the counties west from 
 Chestnut Ridge, attaining its maximum development in Clarion, Arm- 
 strong, Butler, Beaver, and Lawrence, where it is frequently 25 feet 
 thick, or even more, and seldom less than 10 except it has locally 
 thinned away entirely. 
 
 This limestone enters Ohio at Lowellville on the Mahoning River with 
 a thickness of 15 feet, but westward it changes very much from its 
 Pennsylvania type, becoming reduced in thickness, sometimes entirely 
 absent, and occasionally splitting into two beds separated by 15 to 
 50 feet of shales, the lower one of which has been called the Putnam 
 Hill limestone from its occurrence in an eminence of that name at 
 
174 
 
 THE NORTHERN BITUMINOUS COAL FIELD, 
 
 [BULL. 05. 
 
 Zanesville. In one way or another, however, it has been satisfactorily 
 traced by Orton across the Ohio field to where it enters Kentucky from 
 Hanging Kock. 
 
 A layer of flint or u buhrstone” is often incorporated with the top of 
 this bed in Pennsylvania, and the same thing holds true for Ohio, but 
 below this the rock is generally gray for 10 to 15 feet and of great pur- 
 ity, being especially prized as a flux in the smelting of iron ore, and 
 used almost exclusively for this purpose in the Pittsburgh region. The 
 lower portion of the stratum is generally of a bluish color, and its layers 
 are slialy, being interstratified with thin films of clay and other impuri- 
 ties, and occasionally a distinct bed of shale separates the blue layers 
 from the gray above. Hence it seems very probable that, as Prof. 
 Orton once suggested, this shale layer probably increases in thickness 
 through some regions of Ohio, thus separating the upper portion, as the 
 il Gray w limestone, from the io wer or blue part, which has been called the 
 Putnam Hill. On one point, however, in this connection, the writer can- 
 not fully agree with Prof. Orton, and that is concerning the presence 
 of workable coal beds between these two divisions of the limestone. 
 There is certainly none at Zanesville, the typical locality for the Put- 
 nam Hill limestone (Section 104), neither is there any at Shawnee (Sec- 
 tion 105), nor at Kew Lisbon (Section 103), nor Sprucevale (Section 
 102), so that it appears more probable that the supposed workable coal 
 between the two layers of the limestone is founded upon an error in 
 identification. 
 
 Another characteristic of this limestone is that when it becomes thin 
 and impure it almost always exhibits the u cone-in-cone v structure, 
 though there are other horizons in the Coal Measures which show the 
 same feature, notably the Mercer limestones. 
 
 The most northern point at which this limestone has been found in 
 Pennsylvania is in the southern portion of McKean County, where 
 Mr. Ashburner identifies with it a siliceous limestone occurring in the 
 vicinity of Clermont. 
 
 In the Korth Potomac coal basin this limestone has been seen by the 
 writer near Gorman, Garrett County, Maryland, and also below Thomas, 
 along Glady Fork of Black Water. In each case, however, the deposit 
 is entirely difierent from the marine type of western Pennsylvania and 
 Ohio, and resembles more the fresh water limestones under the Free- 
 port coals, since no marine fossils were observed at either locality; in 
 fact there is no point in West Virginia or Maryland where the marine 
 type of this limestone is known to exist, so far as the writer is aware. 
 
 Along the Great Kanawha Kiver, in the vicinity of Cannelton, a bed 
 of siliceous limestone occurs 75 to 100 feet under the Lower Kittanning 
 coal, and it has been identified with the Ferriferous limestone horizon 
 as shown in Section 115. It occasionally exhibits the u cone-in-cone n 
 structure but is not fossil iferous. 
 
 Immediately under the Ferriferous limestone in western Pennsyl- 
 
WHITE.] 
 
 THE CLARION COAL. 
 
 175 
 
 vania there are often 5 to 10 feet of black fossiliferous shales, especially 
 when the limestone is thin or locally wanting, so that the horizon can 
 thus be frequently recognized without the presence of the limestone 
 since the fossils in the shales are practically the same as in the latter. 
 
 THE CLARION COAL. 
 
 Mr. H. Martyn Chance has recently shown (VV, Second Geological 
 Survey of Pennsylvania) that the coal bed which comes so close under 
 the Ferriferous limestone in western Pennsylvania, and was formerly 
 called the Scrub-grass coal, is really an off-shoot from the Clarion, and 
 hence it is unnecessary to retain the name Scrub-grass, which should 
 be replaced with Upper Clarion. 
 
 The main bench of the Clarion coal occurs through western Pennsyl- 
 vania at an interval of 10 to 30 feet below the Ferriferous limestone. 
 Its usual thickness is about 3 feet, though it often swells to 4 or 5. 
 When well developed it generally contains one or two parting slates, and 
 one of them thickening up causes the upper bench to approach the Fer- 
 riferous limestone, and it was then taken for a separate coal by the 
 geologists of the First Pennsylvania Survey, but, as Chance suggests, 
 this should be called the Upper Clarion bed in view of its origin. This 
 upper member is thick enough to mine in only a limited area around 
 the northern outcrop of the same in Clarion, Butler, and Jefferson. Coun- 
 ties. 
 
 The Lower or main Clarion bed is of considerable importance m Penn- 
 sylvania, and generally furnishes some areas of good fuel in nearly 
 every county where its outcrop occurs, though as a rule the coal is 
 rather high in both ash and sulphur. 
 
 In eastern Ohio this bed acquires some importance in the vicinity of 
 Leetonia and New Lisbon, and is there often parted by a vein of tire 
 clay 1 to 4 feet thick, the upper coal alone being mined, and varying in 
 thickness from 2J to 3J feet. Prof. Orton has also shown that the Can- 
 field cannel of Mahoning County belongs to the horizon of the Clarion 
 bed. 
 
 Westward from the eastern tier of Ohio counties, the Clarion coal 
 disappears according to Orton and is of no more importance until Vin- 
 ton and Jackson are reached, but this conclusion is based upon his pres- 
 ent view of the Putnam Hill limestone, which he once regarded as a 
 “ split” from the Ferriferous of Pennsylvania, but which he now ap- 
 pears to reject, since he puts the Clarion coal between this latter lime- 
 stone and the upper or “ Gray” one, and identifies the coal underlying 
 the Putnam Hill limestone as the Brookville bed of Pennsylvania. The 
 writer has elsewhere expressed his doubt of the existence of any work- 
 able coal between these two limestones, believing that the identifica- 
 tions on which the conclusion was founded are erroneous, so that if we 
 substitute Clarion coal for “Brookville” in Prof. Orton’s Ohio series, 
 
176 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 IbulIj. 65. 
 
 all difficulties concerning the disappearance of the Clarion coal between 
 eastern Ohio and Perry County vanishes, and the Clarion becomes one 
 of the regular and persistent beds of the series clear across Ohio as it 
 does in Pennsylvania. In the Zanesville Section (104) the writer has 
 indicated his views as to the equivalency of these members of the Ohio 
 series. 
 
 The Clarion coal attains its maximum thickness in Stark County, 
 Ohio, where it is 6 feet thick and a very fair steam coal, according to 
 Orton. 
 
 In northern West Virginia this bed is generally present in the section, 
 but is usually slaty and too impure to be valuable, so that it has never 
 been mined in that part of the State. 
 
 Section near Eagle, Fayette County , West Virginia . — Along the Great 
 Kanawha Kiver a coal bed, which appears to come at this horizon, has 
 been largely developed for coking purposes in the vicinity of Eagle, 
 Fayette County, and hence is locally known as the Eagle vein. Where 
 best developed there, it varies from 3J to 4J feet in thickness, and is a 
 splendid coking coal, having the following structure in the vicinity of 
 Eagle : 
 
 
 Ft. 
 
 in. 
 
 
 
 Coal 
 
 1 
 
 
 
 
 Shale 
 
 0 
 
 3 I 
 
 Ft. 
 
 in. 
 
 Coal 
 
 0 
 
 - 3 i 
 
 f 4 
 
 9 
 
 Shale 
 
 0 
 
 3 
 
 ! 
 
 
 Coal 
 
 2 
 
 10 J 
 
 
 
 In passing up the Kanawha from Eagle the upper shale parting of 
 this bed gradually thickens till at the mouth of Armstrong Creek, 3 
 miles above, it becomes 20 feet thick and the coal has the structure given 
 in Section 115. 
 
 The interval between this bed and the Lower Kittanning varies be- 
 tween 120 and 200 feet along the Great Kanawha, thickening up to the 
 latter figures at Brownstown (Section 114), but southward from this in 
 Wyoming County the interval swells still further to 230 feet in the vi- 
 cinity of Oceana, as shown in Section 117, w T here the coal in question 
 has a thickness of 5 to 6 feet and is known as the “ coking w vein. 
 There is evidently a wide area of this coal between the Kanawha and 
 Big Sandy Bivers in which it will prove a valuable coking coal. 
 
 A bed of excellent fire clay often underlies the Clarion coal both in 
 Pennsylvania and Ohio, being second in value only to the Kittanuing 
 clay above, and often rivaling it in thickness. 
 
 The interval below the clay down to the next coal bed (Brookville) 
 varies greatly both in thickness and in the rock material which occu- 
 pies it. Occasionally the series ends with the Clarion underclay, which 
 rests immediately on top of the next lower or Conglomerate Measures, 
 while again, shales and a sandstone termed by Chance the Clarion 
 sandstone occupy this interval, which in Pennsylvania is seldom more 
 than 30 to 50 feet thick. 
 
WHITTS. J 
 
 THE EAGLE LIMESTONE. 
 
 177 
 
 In Ohio the interval below the Clarion clay down to the top of the 
 Pottsville Measures is seldom more than 30 feet, the same being true 
 in northern West Virginia, as may be seen from Sections 96 and 97. 
 
 On the Great Kanawha River the internal from the Clarion or Eagle 
 coal down to the top of the Pottsville Measures thickens to nearly 300 
 feet, and consists of a succession of shales and sandstones, in which 
 occur two thiu limestones and two or three thin coal beds. Rone of 
 the latter attain a thickness of 3 feet, however, anywhere between the 
 Kanawha and Big Sandy Rivers, so that the workable coals of this 
 series in that region really end with the Clarion (Eagle) bed. 
 
 Two or three rocks in this interval of 300 feet in southwestern West 
 Virginia require more particular notice. One of them, and the upper- 
 most, is a very pure seam of coal, which at Eagle comes only 20 feet 
 below the main Eagle bed, and is 1J feet thick. I have termed it the 
 Little Eagle coal, since it is possibly a “ split” from the main bed 
 above. To the south it appears to be quite persistent, since it occurs 
 in Wyoming County in every section; but the interval separating it 
 from the Eagle bed has there swelled to 65 feet (Section 117) and the 
 coal has thickened to 27 inches of the same excellent fuel as on the 
 Kanawha. 
 
 THE EAGLE LIMESTONE. 
 
 Another rock worthy of mention in this Kanawha series is an impure 
 limestone which occurs near Eagle at an interval of 75 feet under the 
 Eagle coal. It is only about 1 foot thick, quite dark, fossiliferous, and 
 exhibits the “ cone-in-cone” structure to a wonderful degree, being 
 locally known as u black marble.” The stratum is immediately under- 
 laid by dark shales, which are crowded with marine fossils of the same 
 type as those found in connection with the Ferriferous limestone in 
 Pennsylvania and Ohio ; in fact, so many of the species are identical, and 
 the limestone itself so closely resembles the Ferriferous when thin, that 
 sometimes I have been inclined to think that the two beds may possibly 
 be identical, though this would seem to be impossible from the structure 
 of Section 115, in which the whole lower coal series is exposed both 
 above and below this stratum. If it should turn out to be identical 
 with the Ferriferous, however, then the Eagle coal would be the Lower 
 Kittanning, instead of the Clarion, and the Campbell’s Creek bed the 
 Middle Kittanning, or Neisonville seam of Ohio, instead of the Lower 
 Kittanning. The reader will understand the difficulty of correlation 
 when he remembers that the lower coal series is less than 200 feet thick 
 in the Hocking Valley, Ohio, while here, only 120 miles southward, the 
 same series has swelled out to 1,000 feet. 
 
 The fossiliferous type of the limestone and its accompanying fossilif- 
 erous shale have never been seen by the writer, except in the vicinity 
 of Eagle, and hence I have preferred to regard it as a local deposit 
 below the horizon of the Ferriferous, since the fossils of the Lower Coal 
 Measures have the same general facies at all horizons. 
 
 Bull. 65 12 
 
178 THE NORTHERN BITUMINOUS COAL FIELD. [bull. 65. 
 
 THE BROOK VILLE COAL. 
 
 At the very base of the Lower Coal Measures, except the intervening 
 underclay, there occurs in Jefferson, Clarion, and some other counties 
 of Pennsylvania, a bed of usually slaty and otherwise impure coal, 
 which was long ago named the Brookville bed, from its supposed occur- 
 rence near the town of that name in Jefferson County. This coal ac- 
 quires some local importance around the northern margin of the coal 
 field in Jefferson, Clarion, Butler, and Mercer Counties, but southward 
 and westward it thins away and is often absent even as an impure bed, 
 there being no coal whatever at this horizon where the Pennsylvania 
 series enters Ohio 5 and if I am correct in identifying Prof. Orton’s 
 “Brookville” coal, (Yol. V, Ohio Geology) with the Clarion of Penn- 
 sylvania, then the Brookville coal is generally absent, or at least sel- 
 dom workable anywhere in that State. 
 
 Yery frequently the Brookville coal is represented in Pennsylvania 
 by only a bed of black slate or coaly shale, resting on the top of the 
 Conglomerate Measures, and this is the case in northern West Yirginia, 
 there being no workable coal at this horizon anywhere in that State, so 
 far as the writer is aware. Even in the Kanawha field, where this 
 lower portion of the column is so greatly thickened, the largest coal 
 bed referable to the Brookville horizon is the one in the Wyoming 
 County section (117), and this is only 22 inches. 
 
 On the Great Kanawha a bed of very bituminous shale (Section 115), 
 from which lubricating oil was once manufactured, may possibly repre- 
 sent the Brookville coal horizon, since it is the lowest bituminous 
 stratum in the series there. 
 
 Below this coal in Pennsylvania, and resting immediately on the top 
 of the Conglomerate series, there is sometimes a good bed of fire clay, 
 and Mr. Chance refers to this horizon the clay which is mined so ex- 
 tensively in Clearfield County, at Blue Ball, Wallaceton, and other 
 points along the line of the Tyrone and Clearfield Railroad. 
 
CHAPTER VI. 
 
 THE POTTSVILLE CONGLOMERATE SERIES. 
 
 THICKNESS, CHARACTER, AND EXTENT. 
 
 Beneath the lowest member of the last described series there comes 
 in a group of rocks (No. XII) which are nearly always so different from 
 those in any other portion of the Carboniferous system that all geologists 
 have regarded them as worthy of being placed in a distinct series. To 
 this series several names have been given. * The early geologists of 
 Pennsylvania called it the “ Serai” or “Great” Conglomerate, while in 
 Virginia it has generally been named the No. XII Conglomerate, or 
 simply No. XII. Prof. Lesley has in recent years, however, given it 
 the geographical designation of Potts ville Conglomerate, from the great 
 development of the series near the town of that name, while Prof. Fon- 
 taine, following the Pennsylvania custom of naming the several coal 
 series after prominent rivers along which the beds are exposed, has 
 suggested the name New River series, from that region of West Vir- 
 ginia where its coal beds attain a great development. 
 
 But since only one geographical name is admissible for the series, 
 and as the term Pottsville is now so well ingrafted upon geological 
 nomenclature through the numerous reports of the Second Geological 
 Survey of Pennsylvania, it is thought best to retain it for the series, 
 and at the same time retain New River for the name of the coal group 
 which attains such prominence along that stream, thus putting it on a 
 par with the Mercer group, which occurs in the upper portion of the 
 series. 
 
 As exhibited everywhere in Pennsylvania and West Virginia, this 
 series is very sharply set off from the Lower Coal Measures above and 
 the Lower Carboniferous below, since in both cases there is a great 
 chauge in the lithology, so that the geologist finds no difficulty in deter- 
 mining where the Pottsville series begins as well as where it ends. 
 
 The series as a whole possesses a large amount of hard, white, or 
 grayish white sandstone, much of which is often conglomeritic. The 
 sandstones are harder, more compact, and siliceous than any in the 
 Lower Coal Series above. Bowlders of these sandstones take a smooth 
 polish when rolled along river beds, but this is not the case with most 
 sandrocks above this horizon. 
 
 The fossil contents are also different from those of any sandstones 
 above, since here for the first time in descending the column of rocks 
 
 179 
 
[bull. 65 . 
 
 180 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 do we find sigillarise and the large lepidodendra very abundant in 
 sandstones. 
 
 At the base of the series the change in lithology and life remains is 
 even more abrupt, since with the disappearance of the white or gray 
 sandstones and conglomerates, limestones, red shales, and green mica- 
 ceous sandstones appear, in which plant remains are rare and the fossil 
 trees are all small. 
 
 The Pottsville being composed mainly of very hard sandstones, the 
 grains of which are cemented by silica and peroxide of iron, becomes 
 almost indestructible by ordinary atmospheric influences, and has thus 
 proved a most important factor in determining the topography of the 
 Carboniferous system. Whenever these beds come to the surface in 
 West Virginia and Pennsylvania, wild and rugged scenery is sure to 
 be found. Eapid rivers, high waterfalls, great cliffs, and barren re- 
 gipns generally, mark the lines where these rocks emerge to daylight. 
 The loftiest peaks of the Alleghany Mountains owe their origin to this 
 friendly mantle, while its upturned edges have p r eserved many coal 
 basins from complete destruction. The deep gorges, narrow canons, 
 and wild scenery of the Alleghany, Youghiogheny, Cheat, Mononga- 
 hela, New, Guyandotte, and JBig Sandy Rivers are all carved out of 
 these rocks. The Falls of the Yough, Cheat, Tygart’s Valley, Kanawha, 
 and the “Roughs” of the Guyandotte and Big Sandy are all made by 
 these same beds. 
 
 It was formerly supposed that a vast sheet of pebbly material under- 
 laid all of the true Coal Measures, and that it was destitute of coal ; 
 but the recent work of the Second Geological Survey of Pennsylvania 
 has shown that the series is very complex, consisting of several distinct 
 sandstone members, between which occur shales, several coal beds, and 
 occasionally some limestone. 
 
 In Ohio it happens that the upper members are not so massive as in 
 Pennsylvania or West Virginia, while the coal beds which are promi- 
 nent only around the margins are well developed there, so that the 
 Ohio geologists have classed the upper portion with the Lower Coal 
 Measures, and retained only the lowest member of the series, viz, a 
 stratum termed the Sharon Conglomerate, as the representative of the 
 whole series elsewhere. I shall show in the following pages that the 
 whole series is easily recognized in Ohio, and that the western Penn- - 
 sylvania type of these measures can be traced across Ohio, and hence < 
 for the sake of uniformity in nomenclature the Ohio geologists should 
 cut off 100 to 150 feet from the bottom of their Lower Coal Measure 
 column and combine it with the Sharon Conglomerate below, thus 
 making several members for the series instead of a single stratum. . 
 
 The coals of the Pottsville :>eries, unlike those in the measures above, - 
 are persistent and valuable only around the margins of the Appalachian 
 coal field, and for the most part only where their outcrops are above 
 the level of the principal drainage streams, so that the conditions for- 
 
BULLETIN NO. 05 PL. 
 
 THE POTTSVILLE CONGLOMERATE TOPOGRAPHY IN BLACKWATER CANYON, TUCKER COUNTY, WEST VIRGINIA. 
 
v' . .. 
 
 THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
 
WHITE.] 
 
 THE POTTSVILLE CONGLOMERATE. 
 
 181 
 
 merly supposed to apply to the Lower Goal Measures do actually pre- 
 vail with reference to the coal in this series, since hundreds of carefully 
 kept well records testify to the absence of any workable coal beds in 
 this series over all except the outer rims of the Appalachian field. 
 This same fact is visible to the eye in passing inward toward the center 
 of the field down any one of the great rivers which drain into the Ohio. 
 The Sharon coal disappears southward along the Shenango and Mahon- 
 ing rivers long before its horizon dips down to water level] the New 
 River coals fade out of the section before their outcrops touch the 
 stream to the north ; the great bed at Pocahontas does not extend in- 
 definitely down the Guyandotte and Tug rivers, but only 20 to 30 miles, 
 until it dwindles away to a bed too thin to mine, so that should a shaft 
 be sunk to these beds 30 or 40 miles from their southern or northern 
 outcrops respectively, the same massive, pebbly, white sandstones 
 would be found, but instead of inclosing valuable coal beds they would 
 hold only thin streaks of coal and some black slates. 
 
 Another peculiarity about these interconglomerate coals is the great 
 difference in quality between those around the southern rim of the Ap» 
 palachian field and those around its northern border, for in western Penn- 
 sylvania and across Ohio they are all open burning, hard, and generally 
 known under the name of “ block” coals, which can be used in furnaces 
 in the raw state, while to the south, through West Virginia, Virginia, 
 and on into Tennessee and Alabama, these same coals are very soft 
 and tender, always cementing and making good coke. This difference 
 is connected with different conditions of accumulation, there probably 
 being less moisture in the great peat swamps at the north, and the 
 vegetable accumulations taking place not under water, but partially at 
 least in the open air. This much would be indicated by the innumer- 
 able films of mineral charcoal which characterize the northern coals 
 and render them non-cementing. To the unequal rate of subsidence on 
 the two sides of the Appalachian basin is doubtless owing the condi- 
 tions which brought about the difference in the character of the coals. 
 
 Another peculiarity is the great purity of these early formed coals, 
 their freedom from injurious quantities of ash and sulphur, both at the 
 north and south. This also appears to be due to the conditions attend- 
 ing their deposition rather than to any difference in vegetable tissues, 
 since just previous to the spread of these early coal marshes the whole 
 Appalachian region was sheeted with a thick layer of clean gravel and 
 white sand, thus effectually covering up the muddy deposits of a former 
 epoch and causing the streams which drained into the peat bogs of that 
 time to be pure and clear like our own mountain brooks of the present. 
 
 The thickness of the Pottsville series varies greatly in different por- 
 tions of the Appalachian basin. In the bituminous regions of Penn- 
 sylvania, and everywhere in Ohio, they rarely exceed 300 feet and sel- 
 dom go below 150] but south westward through West Virginia they 
 begin to swell out, reaching 700 feet at the head of Black Water, in 
 
182 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Tucker County ; 1,400 on the New River in Fayette, and probably 
 1,800 at the Kentucky line on the Tug River, in McDowell. Map Sec- 
 tion C will exhibit the manner and rate at which these beds thicken 
 southeastward from their northwestern outcrop in Ohio. The data for 
 its construction were obtained from surface measurements aud oil-well 
 borings, several of which have been recently made along the Great 
 Kanawha. 
 
 This series is also the repository of much salt water, as well as some 
 oil and gas. The celebrated brines on the Great Kanawha, as well as 
 at Pomeroy and many other localities along the Ohio Kiver, come in its 
 basal members, while the “first gas sand” of the Cannonsburg and 
 Hickory region of Washington County, Pennsylvania, is found in the 
 upper half of the same. This rock is also gas-bearing near Glover’s 
 Gap, on the Dodd farm, and near Mannington, Marion County, West 
 Virginia, on the Snodderly farm. 
 
 We shall now give a number of sections in different portions of the 
 Appalachian field, illustrating the character and thickness of the Potts- 
 ville series, and, as with the Lower Coal Measures, shall begin at the 
 northeastern end of the field aud proceed south westward to the Ken- 
 tucky line. 
 
 Section in Fox Township , Elk County , Pennsylvania. — The following 
 section (Fig. 122) exhibits the structure of these beds in Fox Township, 
 Elk County, Pennsylvania, as given by Ashburner (Keport RR, p. 186, 
 Second Geological Survey of Pennsylvania) : 
 
 Fig. 122.— Section 
 in Fox Town- 
 ship, Elk Coun- 
 ty, Pa. 
 
 Fox Township, Elk County, Pennsylvania. 
 [See map, D r.] 
 
 1. Sandstone, Homewood 
 
 ( Coal 
 
 1 6late, black 
 
 Coal 
 
 Slate, black 
 
 Coal 
 
 3. Slate and fire clay 
 
 ( Coal 
 
 4. Coal < Slate 
 
 (Coal 
 
 5. Sandstone Conoquenessing 
 
 6. Shale and slate 
 
 7. Conglomerate 
 
 8. Shales of Ho. XI 
 
 1 ' 2 " 
 O' 3" 
 V 6" 
 0' 3" 
 1 ' 6 " 
 
 1 ' 8 " 
 3' 0" 
 1' 3" 
 
 Ft. in . 
 35 
 
 4 8 
 
 15 
 
 5 11 
 
 50 
 
 10 
 
 50 
 
 Total 
 
 170 7 
 
 As will be observed, the series is thin iu this region, and it seems to 
 decrease still more in Tioga County further to the northeast, where it is 
 less than 100 feet and all in one solid bed. 
 
 Section at Clearfield , Clearfield County , Pennsylvania. — At the town 
 of Clearfield, in the county of the same name, a well was once bored for 
 salt. It begins near the top of these measures, aud the record shows the 
 following structure (Fig. 123), as given in Report H, Second Geological 
 Survey of Pennsylvania : 
 
WHITE.] 
 
 
 Fig. 123.— Section at 
 Clearfield, Clear- 
 field County, Pa. 
 
 Fig. 125. — Section 
 near Patton Sta- 
 tion, Clarion 
 County, Pa. 
 
 THE POTTS VILLE CONGLOMERATE 
 
 183 
 
 Clearfield , Pennsylvania, from boring . 
 
 I See map, E s.J 
 
 1. Sandstone, ferruginous 
 
 2. Sandstone, brown 
 
 3. Sandstone, light colored 
 
 4. Sandstone, coarse, iron-stained 
 
 5. Slate, black, mixed with sand 
 
 6. Sandstone, iron-stained, crumbly 
 
 7. Slate, soft gray 
 
 8. Sandstone, iron-stained, crumbly 
 
 9. Sandstone, white - 
 
 10. Sandstone, grayish white 
 
 11. Slate, dark 
 
 12. Sandstone, light gray 
 
 13. Shales, and red beds of No. XI. 
 
 Ft. 
 
 96 
 
 4 
 
 37 
 
 13 
 
 50 
 
 15 
 
 73 
 
 Total. 
 
 288 
 
 Section near Brookville, Jefferson County , 
 Pennsylvania . — In the vicinity of Brook- 
 ville, Jefferson County, Pennsylvania, 
 these beds exhibit the following structure 
 (Fig. 124), as learned from surface obser- 
 vations combined with the record of the 
 Brookville Gas Company’s well No. 2 : 
 
 BrooTcville, Jefferson County , Pennsylvania. 
 
 [See map, Ep.] Ft. in. 
 
 1 Sandstone, massive, Homewood 75 
 
 2. Shales and sandstone 30 
 
 3. Coal f 0 2 
 
 4. Fire clay 5 
 
 5. Sandstone, massive 70 
 
 6. Concealed 10 
 
 7. Sandstone, massive 90 
 
 8. Slate 20 
 
 9. Sandstone, hard 46 
 
 10. Slate 4 
 
 11. Sandstone, hard 22 
 
 12. Red shales of No. XI. 
 
 Total 372 2 
 
 Here the series has thickened consider- 
 ably, and the triple structure of its sand- 
 stones so often found in Pennsylvania be- 
 comes prominent. N o. 4 appears to occupy 
 the horizon of the Mount Savage fire clay. 
 
 Section near Patton Station , Eed Banlc 
 Township , Clarion County , Pennsylvania . — 
 
 
 Fig. 124.— Section 
 near Brookville, 
 
 , Jefferson Coun* 
 
 Near Patton Station, Bed Bank Township, ty, Pa. 
 Clarion County, Pennsylvania, the rocks of this series 
 exhibit the following structure (Fig. 125), according to 
 Mr. H. Martyn Chance (Report VV, p. 116, Second 
 Geological Survey of Pennsylvania) : 
 
 Patton Station, Red Bank Township, Clarion County, Pennsylvania. 
 
 (See map, Eo,] 
 
 1. Sandstone, hard, massive, Homewood 
 
 2. Shale, with a streak of coal 
 
 3. Iron ore bed 
 
 4. Shale 
 
 5. Sandstone 
 
 6. Shale, with kidney iron ore 
 
 7. Sandstone and shale 
 
 8. Shale, with sandy layers and ore bails ... 
 
 9. Sandstone, with interbedded thin shales. 
 10. Red shale. 
 
 Total 
 
 Feet. 
 
 40 
 
 20 
 
 1 
 
 15 
 
 25 
 
 35 
 
 50 
 
 40 
 
 40 
 
 266 
 
184 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. G3. 
 
 Section at Keller sburg, Armstrong County, Pennsylvania. — Is ear Kel- 
 lersburg, Armstrong County, Pennsylvania, these measures have the 
 following structure (Fig. 126), according to Mr. William 
 G. Platt (H 5, p. 194, Second Geological Survey of 
 Pennsylvania) : 
 
 .v.v.v/.v.v. 
 
 
 
 
 
 62' 
 
 ,-,v .-.v.v.v.v 
 
 
 
 / 
 
 
 10 2! 
 10' 
 3', 
 
 d 
 
 
 WM&M 
 
 
 
 III! 
 
 
 
 
 M 
 
 150* 
 
 IJillf 
 
 2'Z'. 
 
 
 10 
 
 
 50' 
 
 
 
 < 174' 
 
 Section at Kellersburg, Armstrong County , Pennsylvania. 
 
 [See map, Fo,] 
 
 Ft. Ft. in. 
 
 1. Sandstone, massive, Homewood 62 1 
 
 2. Shales 5}- 
 
 3. Sandstone 10 j 
 
 4. Coal (Mercer group) 
 
 5. Shales with iron ore 18 
 
 6. Fire clay 3 
 
 7. Shales 3 
 
 8. Sandstone (Connoquenessing) 150 J 
 
 9. Coal (New River group) 0 2 
 
 10. Clay 2) 
 
 11. Shales 10 > 62 
 
 12. Sandstone 50 1 
 
 77 
 
 174 
 
 Total. 
 
 313 
 
 Here two prominent coal horizons are represented by 
 mere streaks, the upper one being that of the Mercer 
 group of western Pennsylvania and Ohio, while the 
 low r er is the Sharon coal horizon of the latter States 
 and the New Eiver group of West Virginia. 
 KdiersFurg^Arm- Section under Pittsburgh , Pennsylvania. — U n d er Pitts- 
 
 strong county, Pa. k ur g]^ Pennsylvania, we learn the structure of this 
 series from the careful record (Fig. 127) of the Jones & Laughlin gas 
 well No. 2, as given in the Pennsylvania Geological Survey, 1886, p. 734 : 
 
 Fig. 127 — Section 
 un dor Pi ttsb urgh , 
 
 Under Pittsburgh, Pennsylvania ; boring. 
 
 [See map, I m.] 
 
 ao' 1. Sandstone, white, massive, Homewood... 
 
 2. Slate, black, trace of coal 
 
 3. Slate, dark, with sand shells 
 
 4. Coal and slate, with white sandstone 
 
 5. Sandstone, grayish white, fine 
 
 6. Coal, coal slate, and white sandstone 
 
 7. Sandstone and black slate 
 
 8. Sandstone, grayish white, slate in center 
 
 9. Sandy shale, dark 
 
 7 °' 10. Coal 
 
 11. Sandy shale, dark 
 
 12. Coal 
 
 13. Sandy shale, dark „ 
 
 14. Sandstone and black slate..- 
 
 15. Slate, black, sandy, trace of coal 
 
 16. Limestone, Lower Carboniferous. 
 
 Feet. 
 45) 
 15 > 
 
 20 j 
 
 18) 
 42 j> 
 10 j 
 
 Feet. 
 
 5 
 
 10 
 
 70 
 
 Trace. 
 
 20 
 
 1 
 
 2 
 
 7 
 
 7 
 
 Total 
 
 207 
 
 Section under Murraysville , Pennsylvania. — Under Murraysville, West- 
 moreland County, Pennsylvania, the structure is thus exhibited (Fig. 
 
WHITE.] 
 
 THE POTTSVILLE CONGLOMERATE, 
 
 185 
 
 128) by the record of the Philadelphia Company’s gas well No. 49, 
 McCutclieon farm, according to William S. Stevenson, 
 assistant superintendent of the company: 
 
 3 y 
 
 5<f 
 
 .Under Murraysville, Westmoreland County , Pennsylvania (boring). 
 
 [See map, I n.] Feet. 
 
 1. Sandstone, gray, hard, close 
 
 2. Slate, black, soft - - 
 
 3. Sandstone, gray, hard, close 
 
 4. Slate, black, soft 
 
 5. Sandstone, gray, hard, close 
 
 6. Slatp, black, soft - 
 
 7. Red shale of No. XL 
 
 9lf 
 
 Total. 
 
 235 
 
 45 * 
 
 Fig. 128. — Section un- 
 der Murraysville. 
 
 Section under W ashington , Pennsylvania . — Under Wash- 
 ington, Pennsylvania, the structure is thus given (Fig. 
 129) by Prof. Linton from the careful record he kept of 
 the Thayer oil well (Geological Survey of Pennsylvania, 
 p. 765, 1886): 
 
 Under Washington, Pennsylvania (boring). 
 
 [See map, J k.] 
 
 Ft. in. Ft. in. 
 
 87 
 
 1 6 
 
 no o 
 
 iio'e* 
 
 ( Sandstone, fine gray 9' ] 
 
 1. Sandstone, ! Sandstone, white micaceous 32' ( 
 
 Homewood . : Sandstone, white and dark mixed. . 17' f 
 
 ( Sandstone, white, fine 29' J 
 
 2. Coal 
 
 3. Sandstone, white, hard, salt water 06 0] 
 
 4. Sandstone, fine, white and dark . . . .* 15 | 
 
 5. Shale, very dark, hard shells 13 ( 
 
 6. Sandstone, white, fine 10 ( 
 
 7. Shale, black. 4 | 
 
 8. Sandstone, white, fine 2 j 
 
 9. Shale, black, and coal 2 
 
 10. Sandstone, close grained 1 
 
 11. Shale and slate 13 > 29 
 
 12. Shale and shells 15 ) 
 
 13. Shale, black, top of Lower Carboniferous beds. 
 
 Total 230 
 
 Here, as at Pittsburgh (Section 127), a careful rec- 
 ord discloses thin representatives of the Mercer and 
 New Eiver coal groups Nos. 2 and 9, re- 
 spectively. 
 
 Section in Broad Top basin , Huntingdon County , Pennsyl- 
 vania. — In the Broad Top basin of Huntingdon County, 
 Pennsylvania, the structure of these beds is as follows 
 (Fig. 130), according to Iteport T 3 , p. 69, Second Geo- 
 logical Survey of Pennsylvania: 
 
 
 Fig. 129. — Section un- 
 der Washington, Pa. 
 
 30' 
 
 Broad Top basin, Huntingdon County, Pennsylvania. 
 
 [See map, 1 1.] 
 
 Fig. 130. — Section 
 in Broad Top 
 basin, flunting- 
 don County, Pa. 
 
 Sandstone, slightly pebbly, nomewood. 
 ‘ ‘ ‘ bed.... 
 
 3. Sandstone, pebbly. 
 
 2. Shales, with a coal bed- 
 
 4. Shales, with a coal 
 
 5. Sandstone, pebbly. . 
 
 Total 
 
 Feet. 
 
 50 
 
 25 
 
 50 
 
 10 
 
 25 
 
 100 
 
 The triple structure of the sandstones with intervening coal horizons 
 
 is noteworthy here. 
 
186 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section near Weliersburg , Pennsylvania. — At the northern end of the 
 Georges Creek or Cumberland coal basin, near Weliersburg, Somerset 
 County, Pennsylvania, these beds show the following 
 structure (Fig. 131) in the gap of Gladden’s Pun, 
 through the easternmost ridge of the Alleghanies : 
 
 143'6* 
 
 Gladden’s linn, Somerset County, Pennsylvania. 
 [See map, L q.] 
 
 Ft. in. 
 
 1. Sandstone, massive, Homewood 
 
 2. Coal, Mount Savage 
 
 3. Fire clay, Mount Savage 7 6 
 
 4. Sandstone, pebbly . .. 125 
 
 5. Sandstone, dark, shaly 10 
 
 C. Shale 1 
 
 C Coal O' 1 
 
 7. Coal < Slate 
 
 ( Coal 
 
 8. Fire clay, impure, sandy 10 
 
 9. Shales, dark, with iron ore 20 
 
 10. Sandstone, massive 35 
 
 11. Red beds of No. XI. 
 
 Ft. in. 
 75 
 4 
 
 143 6 
 
 ... O' 1'') 
 
 ... O' 4" > — . 
 .. 0' 3" ) 
 
 0 8 
 
 65 
 
 Total 288 2 
 
 20 ' 
 
 This section shows the horizon of 
 the famous Mount Savage fire clay to 
 be in the Mercer coal group. No. 4 
 represents the Connoquenessing sand- 
 
 FigTTsl— Section near stones > while No. 7 is probably at the 
 Weliersburg, Pa. horizon of the Sharon coal. 
 
 Section near Piedmont and Westernport , Mineral County , 
 West Virginia.— The Pottsville conglomerate beds 
 thicken very rapidly in passing southward from the 
 Pennsylvania line through Maryland and West Virginia 
 along the Alleghany Mountain region. This is shown 
 by the following section (Fig. 132), taken on the North 
 Potomac, at Piedmont and Westernport, where that 
 stream cuts through the East Front Eidge of the Alle- 
 ghanies : 
 
 Near Piedmont, Mineral County, West Virginia. 
 
 [See map, N p.l 
 
 Sandstone, massive, Homewood 
 
 Coal 
 
 Shales, dark, containing fossil plants . 
 
 Sandstone, hard, massive 
 
 Shales, and concealed . 
 
 Ft. 
 
 Ft. 
 
 20 
 
 45 1 
 40 I 
 
 30 > 127 
 
 Sandstone, flaggy 10 
 
 Shale 2) 
 
 Coal 1 
 
 Fire clay, dark, sandy 12 ) 
 
 Sandstone, flaggy 10 5 
 
 Coal i. 1 
 
 Shale, with nodular iron ore 2 > 
 
 Shales and flaggy sandstone 40 \ 87 
 
 Sandstone, white, pebbly, very hard 45) 
 
 Shale, with streaks of coal 5 
 
 Concealed shales and sandstones 145 1 
 
 Sandstone, massive 10 j 
 
 Shales, bituminous 10 > 195 
 
 Sandstone, flaggy 10 
 
 Sandstone, massive 20 
 
 Coal 1 
 
 Sandstone 4 
 
 Fire clay and shaio 3 
 
 Sandy shales to top of No. XI red beds 4 
 
 
 145' 
 
 155* 
 
 Total 
 
 473 
 
 Fig. 132.— Section 
 near Piedmont, 
 Mineral County, 
 W. Va. 
 
WHITE.] 
 
 
 $ 
 
 
 
 Fig. 133. — Section a 
 mouth of North Fork c 
 Black Water, W. Va. 
 
 THE POTTSVILLE CONGLOMERATE. 187 
 
 Section on Black Fork of Cheat Elver , Tucker Coun ty , 
 West Virginia . — In Tucker County, West Virginia, 
 50 miles soutli-soutliwest from Piedmont, in tlie gap 
 made by the Black Fork of Cheat Biver through the 
 central portions of the Alleghany Mountains, these 
 beds exhibit a much greater thickness than at Pied- 
 mont, as will be seen by the following section (Fig. 
 133) made there by Mr. James Parsons, chief engi- 
 neer of the West Virginia Central Bailroad : 
 
 Mouth of North Fork of Black Water, Tucker County, West Vir- 
 ginia. 
 
 [See map, P o.] 
 
 1. Sandstone, Homewood 
 
 2. Coal, slaty and bituminous shale 
 
 3. Shale, dark 
 
 4. Sandstone, massive, pebbly 
 
 5. Brown shale 
 
 6. Coal (Nuttall) 
 
 7. Shale, drab 
 
 8. Sandstone, massive 
 
 9. Shales with iron nodules 
 
 10. Fire clay 
 
 11. Shale 
 
 12. Sandstone, fine grained, flaggy 
 
 13. Shale 
 
 14. Coal 
 
 15. Shale 
 
 16. Sandstone, massive 
 
 17. Sandstone and shales 
 
 18. Coal 
 
 19. Shale, brown 
 
 20. Coal. 
 
 21. Bituminous shale, with coal streaks 
 
 22. Brown shale e 
 
 23. Coal 
 
 24. Bituminous shale, with coal streaks 
 
 25. Shale 
 
 26. Sandstone, massive 
 
 27. Shale, brown 
 
 28. Red beds, top of No. XI. 
 
 Ft. in. Ft. in. 
 
 40 
 
 9 
 
 228 
 
 26 
 
 16 
 
 47 
 
 28 
 
 2 
 
 4 
 
 39 
 
 6 
 
 j 263 
 2 6 
 
 , 142 
 
 
 24 
 
 65 
 
 43 
 
 0 
 
 22 
 
 1 
 
 6 
 
 26 
 
 1 
 
 3 
 
 32 
 
 35 
 
 20 
 
 0 6 
 
 1 
 
 132 
 
 2 
 
 59 10 
 
 Total 733 10 
 
 Here we find the entire interconglomerate coal 
 group represented. No. 2 comes apparently at the 
 Mercer horizon and is the u Railroad” vein along the 
 Potomac. 
 
 No. G comes at the horizon of the Nuttall bed of New 
 Biver, while Nos. 14 to 24 represent the lower ones 
 t along that stream as well as the great Pocahontas vein 
 of McDowell and Mercer Counties, West Virginia. 
 
188 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [bull. 65, 
 
 Section near Rowlesburg , West Virginia. — A fine section of the Con- 
 glomerate coals is exposed in the cuts of the Baltimore and Ohio Rail- 
 road, near the summit of Cheat River grade, 4 miles west from Rowles- 
 burg, Preston County, West Virginia (Fig. 134) : 
 
 £»' 
 
 Along the Baltimore and Ohio Bailroad, Cheat River grade, four 
 miles west from Rowlesburg, Preston County, West Virginia. 
 
 
 BS * 
 
 
 
 
 
 [See map, N n.] 
 
 1. Sandstone, massive, coarse, yellowish, Homewood 
 
 C Coal O' 
 
 2. Coal < Shales, sandy 
 
 (Coal... O' 
 
 3. Shales, brown, sandy 
 
 4. Coal, slaty 
 
 5. Shales 
 
 6. Sandstone, massive 
 
 7. Sandstone, flaggy 
 
 8. Sandstone, massive, grayish white 
 
 9. Sandstone, flaggy 
 
 10. Shales, brown 
 
 11. Sandstone, grayish white 
 
 12. Shale, brown 
 
 ' 5 ") 
 
 ' O'A 
 
 ' 5 " ) 
 
 Ft. in. 
 
 Ft. in. 
 60 
 
 6 10 
 
 45 
 
 2 
 
 13. New River coal beds. 
 
 Coal 
 
 . . O' 5" 
 
 Shale, gray - 
 
 .. 4' 0" 
 
 Coal I 
 
 .. 0' 4" 
 
 Shales, drab, sandy. . 
 
 .. 8' 0" 
 
 Iron ore 
 
 .. O' 6" 
 
 Shales 
 
 , . 5' 0" < 
 
 Coal 
 
 .. 1' 0" I 
 
 Shales 
 
 .10' 0" | 
 
 Coal 
 
 .. 0' 4" I 
 
 Shales, brown, sandy. 25' 0" 
 
 Coal 
 
 .. 0' 6" J 
 
 6 J 
 
 3S f 
 
 14. Shales, brown 
 
 15. Sandstone 
 
 16. Shales, buff, sandy 
 
 17. Sandstone, massive, pebbly 
 
 18. Concealed, and shales 
 
 19. Top of No. XI, red shales. 
 
 Total. 
 
 55 1 
 
 95 
 
 362 5 
 
 Nos. 2 and 4 represent the Mercer coal group, Nos. 
 fig. 134 .— Section near ^ ^ the Connoquenessing sandstones, while No. 
 
 Rowlesburg, w. Va. 13 represents the New River coal group. 
 
 Section near mouth of Sandy Creeh, Preston County , West Virginia . — 
 Farther northwest, down Cheat River, and in the center of the Ligonier 
 basin, the Pottsville series exhibits the following struc- 
 ture (Fig. 135) near the mouth of Sandy Creek, Preston 
 County, West Virginia : 
 
 Near mouth of Sandy Creek, on Cheat River, Preston County, West 
 
 Virginia. 
 
 [See map, M m. J 
 
 Ft. 
 
 1. Sandstone, massive, very pebbly near middle 
 
 2. Shales, dark. 
 
 3. Coal 
 
 ( Coal 
 
 O' 
 
 10" i 
 
 { Shale 
 
 0' 
 
 3" > 
 
 ( Coal 
 
 0' 
 
 5"$ 
 
 Ft. in. 
 160 
 .10 
 
 1 6 
 
 Fig. 135. — Section 
 nearmouth ofSaudy 
 Creek, Preston 
 County, W. Va. 
 
 4. Fire clay 7) 
 
 5. Slate, black, fissile 15 > 37 
 
 6. Sandstone, gray 15 ) 
 
 7. Shale, with streak of coal 1* 
 
 8. Sandstone, grayish white 15 
 
 9. Green and red shales of No. XI. 
 
 Total 224 6 
 
 Here, as frequently happens, the Mercer coal group 
 disappears entirely, while the Homewood and Conno- 
 quenessing sandstones unite into one solid mass. Nos. 
 3 to 7 represent the New River coal group. 
 
WHITE. J 
 
 THE POTTSYILLE CONGLOMERATE. 
 
 189 
 
 Section on Booth's Creek , Taylor County , West Virginia,— The struc- 
 ture of the Pottsville beds in the region along the line between Taylor 
 and Marion Counties, West Virginia, is learned from a 
 boring made for oil on Booth’s Creek, Taylor County, by 
 Mr. John L. Steele, to whom I am indebted for the fol- 
 lowing record (Fig. 136) : 
 
 Booth's Creek, Taylor County , West Virginia (boring). 
 
 [See map, O 1.] Ft. 
 
 1. Sandstone, hard, wliite, pebbly 159 
 
 2. Black slate - . 15 
 
 3. Shale, gray and sandy 20 
 
 4. Shale, black - 15 
 
 5. Shale, gray, sandy . 20 
 
 6. Sand, gray, pebbiy 10 
 
 7. Bed beds of No. XI. 
 
 Total 239 
 
 Here the structure is very much like that of the pre- 
 vious section on Cheat River, and the thickness is also 
 nearly the same. 
 
 Section under Clarksburg , West Vir- 
 ginia. — Under Clarksburg, Harrison 
 
 County, West Virginia, the succession is 
 given as follows (Fig. 137), from the rec- 
 ord of the Despard gas well, on the authority of Prof. 
 
 T. M. Jackson: 
 
 Clarksburg, West Virginia (gas well). 
 
 Fig. 136. — Section 
 on Booth’s Creek, 
 Taylor County, 
 W. Va. 
 
 
 [See map, Ok.] 
 
 1. Sandstone, black — 
 
 2. Sandstone, white 
 
 3. Sandstone, gray 
 
 4. Sandstone, white — 
 
 5. Sandstone, gray 
 
 6. Sandstone, dark 
 
 7. Shale, black 
 
 8. Sandstone, white 
 
 9. Sandstone, gray . — 
 10. Bed beds of No. XI. 
 
 30 ^ 
 
 Ft. 
 
 174 
 
 Total. 
 
 256 
 
 50' 
 
 U* 
 
 -n> 
 
 i 
 
 Fig. 137. — Section 
 under Clarks- 
 burg, W. Va. 
 
 7 <f 
 
 Section near Farmington , West Vir- 
 ginia. — Under the central portion of 
 Marion County, West Virginia, the 
 structure is shown by the record of the 
 HukiH oil boring near Farmington (Fig. 138), as given 
 in Second Geological Survey of Pennsylvania, 1886 (pp. 
 782, 783) : 
 
 Farmington, West Virginia (oil boring). 
 
 [See map, M 1.] 
 
 Ft. 
 
 1. Sandstone 100 
 
 10 
 
 17 
 
 70 
 
 12 
 
 
 Fig. 138. — Section 
 near Farmington, 
 W. Va. 
 
 2. Shell 
 
 3. Slate 
 
 4. Black slate 
 
 5. Sandstone 
 
 6. Bed beds of No. XI. 
 
 Total 
 
 209 
 
190 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section under Wellsburg , West Virginia. — Under Wellsburg, Brooke 
 County, West Virginia, the Barclay gas well No. 1 gives tlie following 
 (Fig. 139) for these beds on the authority of Mr. Bar- 
 clay : 
 
 
 ijpi 
 
 l llli 
 
 TS!. 
 
 aft' 
 
 14 / 
 
 Wellsburg, West Virginia (gas boring). 
 [See map, J j.] 
 
 1. Sandstone, white 
 
 2. Sandstone, gray . 
 
 3. Sandstone, blue . . 
 
 4. Coal 
 
 5. Slate and shale. . . 
 
 Total. 
 
 Ft 
 
 75 1 
 30 > 
 
 40 j 
 
 Ft. 
 
 145 
 
 31 
 
 182 
 
 ri ?- 13 ^“T, s l ction txt" The coal reported in this section comes at the liori- 
 
 va. zon of the Sharon bed of Ohio and Pennsylvania, but 
 
 it was probably nearly all coaly slate or else a local thickening, since 
 other borings put down in this region do not report it at all. 
 
 Section in Mercer County , Pennsylvania . — Along the northwestern 
 margin of the Appalachian field in the counties of Lawrence and Mer- 
 cer, bordering the Ohio State line, a series of workable coal beds make 
 their appearance in the Pottsville series and extend along the margin 
 of the field clear through to southern Ohio. The general section of the 
 Pottsville series of Mercer County, Pennsylvania, given in Q 3 ( p. 33), 
 Second Geological Survey of Pennsylvania, shows the succession of 
 these coal groups as follows (Fig. 140) : 
 
 Fig. 140 — Section in 
 Mercer County, Pa. 
 
 Mercer County, Pennsylvania. 
 [See map, E k.] 
 
 1. Sandstone, Homewood 
 
 2. Shales .... 
 
 3. Iron ore 
 
 4. Limestone, Mercer, Upper 
 
 5. Coal, Mercer, Upper 
 
 6. Shales 
 
 7. Iron ore 
 
 8. Limestone, Mercer, Lower 
 
 9. Shales 
 
 10. Coal, Mercer, Lower 
 
 11. Shales... 
 
 12. Iron ore 
 
 13. Shales 
 
 14. Sandstone, Connoquenessing, Upper. . 
 
 15. Shales with iron ore — 
 
 16. Coal, Quakertown 
 
 17. Shales 
 
 18. Sandstone, Connoquenessing, Lower. . 
 
 19. Shales, Sharon, iron bearing 
 
 20. Coal, Sharon .' 
 
 22. Fire clay and shales 
 
 23. Sharon Conglomerate, base of Xo. XII 
 
 Total 
 
 Ft. in. 
 
 6 i 
 
 l 
 
 Ft. in. 
 50 
 
 5 
 
 2 
 
 2 6 
 
 44 6 
 
 66 
 
 2 
 
 100 
 
 4 
 
 5 
 20 
 
 301 
 
WHITE.] 
 
 THE POTTSVILLE CONGLOMERATE. 
 
 191 
 
 Section near Quakertown , Mahoning County , Ohio . — Where the Ohio- 
 Pennsylvania State line crosses the Mahoning Eiver, near Quakertown, 
 these beds exhibit the following structure (Fig. 141) : 
 
 Ohio -Pennsylvania line on Mahoning River. 
 
 [See map, Fk;] Ft. in. 
 
 1. Homewood sandstone 
 
 2. Concealed 
 
 3. Limestone, Upper Mercer . 
 
 4. Fire clay 
 
 5. Sandstone, shaly 
 
 6. Coal, slaty, Middle Mercer 
 
 7. Fire clay and sandy shales 
 
 8. Limestone, Lower Mercer 
 
 9. Shales 
 
 10. Coal, Mercer, Lower 
 
 11. Fireclay 
 
 12. Shales, sandy 
 
 13. 
 
 14. 
 
 15. 
 
 Sandstone, Connoquenessing, Upper 45 
 
 Coal, Quakertown 
 
 Fig. 141. — Section near 
 Quakertown, Ohio. 
 
 Fire clay and shales . . . 
 
 Qq ti f\ atoll p ( ImmnmiP. 
 
 [Sandstone 
 
 - jn 
 
 Oaii'ioiinic, v/uiiiunpiC’ 
 
 nessing, Lower 
 
 . ] Sandstone, flaggy 
 
 ... 40' 
 
 
 [Sandstone, massive . - 
 
 ... 30', 
 
 3 6 1 , 
 
 99 
 
 Blue shales, with iron ore halls 20 
 
 Sandstone, massive 10 
 
 Coal, Sharon, and bituminous slate 
 
 Sandstone, flaggy, to base of No. XII 
 
 Total 
 
 Ft. in. 
 20 
 10 
 
 24 5 
 
 55 6 
 
 1 2 
 
 132 G 
 
 1 6 
 
 25 
 
 270 1 
 
 The Sharon coal of these sections (140, 141) represents the New Eiver 
 coal group of West Virginia, since the Mercer group above does not 
 furnish valuable coal in that region, but only thin slaty beds. 
 
 Section in Holmes County , Ohio. — In Holmes County, Ohio, these beds 
 are given as follows (Fig. 142), in Vol. V, Ohio Geology, p. 837 : 
 
 Holmes County , Ohio. 
 
 [See map, H e.] 
 
 Fig. 142.— Section 
 in Holmes Coun- 
 ty, Ohio. 
 
 1. Interval, sandstone and shales 
 
 2. Limestone, Lower Mercer 
 
 3. Coal, Lower Mercer 
 
 4. Concealed 
 
 5. Gray shales 
 
 6. Coal 
 
 7. Gray shale and concealed 
 
 8. Sandstone, Upper Connoquenessing 
 
 9. Coal, Quakertown 
 
 10. Sandstone, shaly, Lower Connoquenessing. 
 
 11. Coal, thin 
 
 12. Sandstone 
 
 13. Coal, Sharon 
 
 14. Fire clay 
 
 15. Lower Carboniferous beds. 
 
 Ft. in. 
 60 
 
 1 G 
 
 17 
 
 6 
 
 2 
 
 23 6 
 15 6 
 blossom 
 33 G 
 
 3 
 
 2 G 
 10 
 
 Total 
 
 174 G 
 
192 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section in Washington County , Ohio. — In Washington County, Ohio, 
 the Pottsville measures are given as follows (Fig* 143) by Mr. F. W. 
 Minshall, from the record of the Epler oil boring : 
 
 Epler oil boring, Washington County , Ohio. 
 
 [See map, M g.J 
 
 1. Sandstone 
 
 2. Shales 
 
 3. Coal 
 
 4. Shales 
 
 5. White, pebbly sandstone .. 
 
 6. Black shales 
 
 7. Lower Carboniferous beds. 
 
 Ft. 
 
 24 
 
 20 
 
 70 
 
 60 
 
 4 
 
 Total 178 
 
 Section at Parkersburg , West Virginia. — The Camden 
 Consolidated Oil Company, in boring at Parkersburg, 
 fig. 143 .— section West Virginia, found the following structure (Fig. 144), 
 CouTty S ohfo ton according to Mr. B. A. Cole, the superintendent: 
 
 Parkersburg , West Virginia (boring). 
 
 [See, map, O f.] 
 
 Ft. 
 
 1. Shales, gray 110 
 
 2. Sandstone, hard, white 50 
 
 3. Slate, black 25 
 
 4. Sandstone, hard, gray 50 
 
 5. Shales of No XT. 
 
 Total 
 
 235 
 
 Section near Burning Springs , West Vir- 
 ginia. — Near Burning Springs, Wirt 
 County, West Virginia, these same beds 
 have this succession (Fig. 145), as found 
 in the Simpson oil boring by Mr. Min- 
 shall : 
 
 Simpson ivell, Wirt County, West Virginia. 
 
 [See map, P g.] 
 
 
 Sflf 
 
 50l 
 
 Fig. 144. — Section 
 under Parkers- 
 burg, W. Va. 
 
 Ft. 
 
 Fig. 145.— Section 
 near B u r n in g 
 prings, W. V a. 
 
 1. Sandstone 
 
 2. Coal 
 
 3. Sandstone 
 
 4. Shales - 
 
 5. Coal - 
 
 6. Sandstone 
 
 7. Shales 
 
 8. Sandstone 
 
 9. Shales 
 
 10. Coal 
 
 11. Conglomerate 
 
 12. Shales - 
 
 13. Limestone, Subcarboniferous. 
 
 Total ,352 
 
 The Burning Springs section (Fig. 145) shows a rapid 
 increase in the thickness of these beds towards the 
 southeast, since they are just twice as thick here as in 
 Washington County, Ohio (Section 143), .50 miles distant. 
 
WHITE.] 
 
 THE POTTSVILLE CONGLOMERATE. 
 
 193 
 
 Section near Jackson Furnace , Jackson County , Ohio. — In Jackson 
 County, Ohio, the Pottsville series has the following structure (Fig. 
 
 146) near Jackson furnace, as given in the Ohio Geo- 
 logical Survey, 1870 (p. 158) : 
 
 Jackson Furnace , Jackson County , Ohio. 
 
 [See map, P b.j 
 
 Ft. in. 
 0 8 
 20 
 
 0 7 
 
 15 
 
 1. Iron ore .1 
 
 2. Interval 
 
 3. Iron ore 1 
 
 4. Coarse sandstone 
 
 5. Coal trace 
 
 6. Shale 18 
 
 7. Iron ore 0 6 
 
 8. Clay, shale 1 1 
 
 9. Sandstone, coarse 20 
 
 10. Sandy shales and laminated sandstone 115 
 
 11. Coal ' . 2 6 
 
 12. Fireclay 2 6 
 
 13. Clay, shale 2 6 
 
 14. White sandstone — 10 
 
 15. Sandy shale 10 
 
 o'ar 1 - _ 1 n A 
 
 16. Coal 
 
 17. Shales and sandstones to base of No. XII 
 
 Total 238 
 
 fig. M6.-Section Section at Hanging Bock , Sciota County , Ohio. — In the 
 iface^j a^k To ii vicinity of Hanging Rock, Ohio, the Pottsville series has 
 
 County, Ohio. 
 
 the following structure (Fig. 147) : 
 
 Fig. 147. — Section 
 at Hanging Rock, 
 Sciota County, 
 Ohio. 
 
 Hanging Bock , Sciota County, Ohio. 
 
 [See map, It a.] 
 
 Ft. in. 
 
 1. Sandstone, massive 
 
 2. Fire clay 
 
 3. Limestone and iron ore, Upper Mercer 
 
 4. Shales 
 
 5. Coal, Upper Mercer 
 
 6. Fire clay, sandy 
 
 7. Sandstone, shaly 
 
 8. Shales, drab 
 
 ( Coal 0' 5 " 1 
 
 9. Coal, Lower Mercer < Fire clay V 4" > 
 
 (Coal 1'4") 
 
 10. Fire clay and shales 
 
 11. Sandstone, Connoquenessing, Upper, massive, coarse, yellowish 
 
 12. Sandy shales and shaly sandstone 
 
 ( Coal O' 5" } 
 
 13. Coal, Quakertown < Slate 0' 3'' > 
 
 ( Coal V 5") 
 
 14. Fire clay 
 
 15. Sandy shales 
 
 16. Sandstone, Lower Connoquenessing, massive 
 
 17. Shales, dark blue, with iron ore 
 
 18. Iron ore, sandy 
 
 19. Blue sandy shales 
 
 20. Interval to base of Pottsville beds under river, from drill hole (E. B. 
 
 Willard) 
 
 40 
 
 5 
 
 1 
 
 20 
 
 0 
 
 2 
 
 8 
 
 8 
 
 5 
 
 30 
 
 15 
 
 3 
 
 17 
 
 25 
 
 5 
 
 1 
 
 40 
 
 40 
 
 4 
 
 1 
 
 1 
 
 Total 
 
 270 6 
 
 Here the Mercer group, together with the Quakertown 
 coal, is distinctly recognizable at the very southern bor- 
 der of Ohio, while the Connoquenessing sandstones and 
 
 the dark blue Sharon iron-bearing shales below look exactly like the 
 same beds in eastern Ohio. The base of , the series was given me here 
 from the record of a bore-hole put down by Mr. E. B. Willard, super- 
 intendent of the Hanging Rock Coal Company. 
 
 Bull 65 13 
 
194 
 
 THE NORTHERN' BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section on Big Sandy River , Lawrence County, Kentucky . — Twenty miles 
 up the Big Sandy River, and near the mouth of Blaine Creek, the suc- 
 cession of the series is as follows (Fig. 148) according to 
 the record of Rigdon gas well No.2, as furnished by Mr. 
 F. H. Oliphant: 
 
 € 
 
 
 v,\ 
 
 Under Big Sandy River at mouth of Blaine Creek (boring). 
 [See map, Y b.j 
 
 Ft. 
 
 25 
 
 5 
 
 20 
 
 25 
 
 15 
 
 20 
 
 20 
 
 40 
 
 Sandstone, white, salt water 100 
 
 10 
 
 10 
 
 90 
 
 25 
 
 10 
 
 30 
 
 1. Sandstone, white 
 
 2. Slate, black 
 
 3. Sandstone, white 
 
 4. Sandstone, dark gray. 
 
 5. Slate, gray 
 
 6. Sandstone, dark 
 
 7. Slate, gray 
 
 8. Sandstone, dark gray. 
 
 10. Sandstone, dark blue 
 
 11. Slate, black 
 
 12. Sandstone, white 
 
 13. Slate, black 
 
 14. Shells 
 
 15. Sandstone, hard blue 
 
 16. Limestone, Lower Carboniferous. 
 
 Total 
 
 445 
 
 This section exhibits the beginning of the great south- 
 eastern thickening of the Pottsville series along the Big 
 Sandy, but we have not sufficient data southward from 
 Blaine Creek to trace the rate of increase along the Tug 
 Fork, since even the top of the Pottsville does not rise 
 to daylight on that stream for 100 miles above the mouth 
 of Blaine. When the bottom series does finally come to 
 the surface at the southern edge of McDowell County, 
 West Virginia, it is not less than 1,500 feet thick, and 
 may possibly be 2,000, since the Kentucky geologists claim the latter 
 thickness for these measures on the headwaters of the Big Sandy. 
 
 There is no point along the Tug River in West Virginia where a 
 vertical measurement can be made ; hence, if the exact thickness is 
 ever determined it must be by a boring. 
 
 The black slates, Nos. 2, 11, and 13 of the above section, probably 
 represent the interconglomerate coal beds. 
 
 Fig. 148.— Section 
 under Big Sandy 
 Biver near mouth 
 of Blaine Creek. 
 
WHITE.] 
 
 THE POTTSVILLE CONGLOMERATE. 
 
 195 
 
 Section under Charleston , Kanawha County , West Virginia . — On the 
 Great Kanawha River some recent borings for gas have supplied the 
 necessary data there, thus giving measurements at two 
 points before the whole formation comes to the surface. 
 The first one of these is the record of the Edwards gas 
 well Ko. 3, bored at Charleston, West Virginia, which 
 gives the following structure (Fig. 149) for these beds, 
 according to Mr. William S. Edwards : 
 
 
 
 
 
 
 
 
 
 
 
 
 ^;v;vav 
 
 
 
 
 
 
 
 •/.V.v.y/v.Y. s 
 
 
 
 V- 1 3 
 
 \ \ \ •. ’. li 
 
 
 
 
 y.w.v v/.v.v 
 
 
 
 : ;’v3r3^Sv 
 
 
 -1:. d” 
 
 Under Charleston , Kanawha County, West Virginia (boring). 
 [See map, T f.] 
 
 1. Sandstone 
 
 2. White sandstone 
 
 3. Hard sandstone and shells 
 
 4. White sandstone 
 
 5. Black sandstone and shell 
 
 6. White sandstone 
 
 7. Hard sandstone 
 
 8. Hard black shells and gas 
 
 9. White sandstone 
 
 10. Black sandstone 
 
 11. White sandstone 
 
 12. Black sandstone 
 
 13. White sandstone 
 
 14. Hard shells 
 
 15. White sandstone 
 
 16. Sandsheil, hard 
 
 17. White sandstone 
 
 18. Black sand 
 
 19. Lower Carboniferous limestone 
 
 Total 
 
 Ft. 
 
 20 
 
 30 
 
 65 
 
 45 
 
 30 
 
 20 
 
 55 
 
 90 
 
 55 
 
 10 
 
 10 
 
 15 
 
 5 
 
 10 
 
 25 
 
 10 
 
 75 
 
 10 
 
 580 
 
 Here the Pottsville series has thickened to about three 
 times its size at the northwestern outcrop of these beds 
 in Ohio, 100 miles distant. Whether the thickening is 
 gradual or abrupt is not known, and can not be until 
 more borings are made. It is probably gradual from 
 the center of tbe great Apalachian trough, 50 miles 
 northwest of Charleston. 
 
 The interconglomerate coal beds appear to be entirely 
 
 ^der^cirfries^oS’ al)seut fr° ra tlie a 5ove section, since not even black 
 Kanawha County’, slates are present according to the driller’s record. 
 
196 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65. 
 
 Section at Burning Spring, Kanaivha County , West Virginia . — At Burn- 
 ing Spring, 9 miles south from Charleston, the record of Edwards gas 
 well No. 1 gives these beds as follows (Fig. 150) : 
 
 
 ii® 
 
 w 
 
 $ 176' 
 
 yXvXtfv 
 
 *>> 
 
 VV.V 
 
 
 
 
 
 Xv.-.v.'.' 
 
 
 
 
 >AVAV.V 
 
 w,v 
 
 ^•XVA 
 
 
 Y/S/.yV. 
 
 ;‘vX 
 
 ’•.y.v.v 
 
 
 
 
 iv.v-v.X 
 
 
 .v.'.v.v.v.w. 
 
 f.v.v.’.v.v.v. 
 
 
 
 
 »,*.*-*• vv.v.v; 
 
 Burning Spring, Kanawha County , West Virginia (boring). 
 [See map, Tf.] 
 
 1. Sandstone, hard white 
 
 2. Coal, hard 
 
 3. Sandstone, hard white, salt water 
 
 6. Slate, black 
 
 7. Sandstone, hard white 
 
 8. Sandstone, blue hard 
 
 9. Limestone, Lower Carboniferous 
 
 Ft. 
 
 Ft. 
 
 
 176 
 
 
 6 
 
 . 200 . 
 
 
 * 100 ( 
 
 555 
 
 255 ^ 
 
 2 
 
 
 50 
 
 
 50 
 
 
 . 839 
 
 No. 2 represents the Mercer coal group, though no 
 coal thick enough to mine ever occurs’at this horizon 
 to the southward, where these beds rise above water 
 level. 
 
 The New River coals belong in Nos. 4 and 6 of the 
 section, but they here contain no coal whatever, though 
 only 40 miles north from the New River coal field. 
 
 The series has here increased 259 feet in thickness 
 in 9 miles, a very rapid rate, and possibly indicating 
 that the great thickness (580 feet) found under Charles- 
 ton may have been abruptly instead of gradually ac- 
 quired. • 
 
 In this boring a considerable flow of natural gas 
 was obtained in the top of the Pocono sandstone, or 
 “Big Injun” oil sand, at a depth of about 1,000 feet. 
 This is the locality where natural gas was first used 
 for manufacturing purposes in the United States, as 
 far back as 1841. It was utilized for 
 evaporating salt water. One of the gas 
 wells found here, according to report, 
 displaced for fuel 2,000 bushels of coal 
 daily during a period of ten years. The 
 last well, however (bored in 1887), does 
 not produce much over 500,000 cubic 
 feet of gas daily. The most productive 
 wells were situated near the crest of the 
 anticline which crosses the Kanawha 
 River at Burning Spring. 
 
 ITig. 150. — Section at Burning Spring, 
 Kanawha County, W. Va. 
 
WHITE.] 
 
 THE POTTSVILLE CONGLOMERATE, 
 
 197 
 
 no' 
 
 17Q 4 
 
 
 IjSff 
 
 Section near Nuitallburg , Fayette County , Virginia . — Passing on 
 
 southward up the Kanawha and New Rivers, there is no opportunity 
 
 to get another measurement of the 
 Pottsville series until all of its mem- 
 bers have risen above the level of New 
 River, in the vicinity of Nuttallburg, 
 Payette County, W est Virginia, 50 miles 
 distant from Burning Spring, where 
 the following succession occurs (Fig, 
 151): 
 
 Vicinity of Nuttallburg , Fayette County , West 
 Virginia. 
 
 [See map, U h.] 
 
 . 
 
 I2Q’ 
 
 360 " 
 
 
 4*sT 
 
 aa* 
 
 40 ' 
 
 <*4% 
 
 IQ 
 
 ■arf 
 
 
 140’ 
 
 420 
 
 Fig. 
 
 151.— Section in vicinity of Nuttall- 
 burg. Fayette County, W. Va. 
 
 2. Shales 
 
 3. Coal 
 
 4. Sandy shales and sandstone . 
 
 5. Sandstone 
 
 6. Black slate 
 
 7. Coal 
 
 8. Shales and sandstone 
 
 9. Coal 
 
 10. Shales, sandstone and shales. 
 
 11. Coal, Nuttall 
 
 12. Shales and slates 
 
 14. Slates, dark 
 
 15. Concealed, and shales 
 
 16. Coal, Fire Creek 
 
 17. Shales and sandstone 
 
 ( Coal 
 
 I Slate 
 
 18. Coal,Quinnimont (?) •( Coal 
 
 1 Slate 
 
 Coal 
 
 Ft. 
 
 le- l 
 
 Ft. 
 
 in. 
 
 
 170 
 
 
 .. 75) 
 
 1 
 
 
 " ll 
 
 102 
 
 
 
 1 
 
 
 
 75 
 
 
 
 0 
 
 10 
 
 
 50 
 
 
 .. 75) 
 
 3 
 
 6 
 
 . . 155 { 
 
 jsJ 
 
 360 
 
 
 
 3 
 
 6 
 
 ,.. V 0") 
 .. . O' 3” I 
 ,.. 2' 0" 
 ...O' 2" \ 
 ... r 0" J 
 
 130 
 
 
 4 
 
 5 
 
 420 
 
 19. Shales and sandstone 
 
 20. Coal, slaty 
 
 21. Shales 
 
 22. Coal 
 
 23. Shales 10 ] 
 
 24. Concealed 30 
 
 25. Sandstone, mastive 125 | 
 
 26. Concealed, and sandstone 60 
 
 27. Sandstone, massive 140 1 
 
 28. Concealed, and sandstone to top of 
 
 No. XI shales „... 55 J 
 
 Total 1,400 0 
 
 No. 11, the Nuttall coal, is the highest 
 member of the New River group that 
 ever furnishes valuable coal along that 
 stream. Its place in the Pottsville 
 series is 400 feet below the top, and the 
 other thin coals above it belong to the 
 Mercer group. 
 
 Whether No. 18 is identical with the 
 Quinnimont,or whether this latter coal 
 is the same as the Fire Creek, No. 16, 
 are questions yet unsettled. 
 
 Just what represents the Pocahontas 
 coal of McDowell and Mercer Counties 
 in this section, or whether it is repre- 
 
 sented at all is uncertain, but No. IS may possibly come at that horizon. 
 
198 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [DULL. 65. 
 
 Section on Crane Creelc, Mercer County, West Virginia . — At the ex- 
 treme southern edge of the Appalachian field in Mercer County, West 
 
 Fig. 152. —Section on Crane Creek, Mercer 
 County, W. Ya. 
 
 Virginia, the following section (Fig. 152) 
 of the Pottsville series was obtained 
 upon the waters of Crane Creek by add- 
 ing 400 feet to the summit of the column 
 for the estimated thickness of beds re- 
 moved by erosion : 
 
 Crane Creek, Mercer County, West Virginia. 
 
 [See map, Y g. ] Ft. Ft. in. 
 
 1. Sandstones and shales, here eroded from 
 
 top of No. XII (estimated) 
 
 2. Shales and sandstones 
 
 3. Sandstone and shales 
 
 4. Sandstone, gray 
 
 5. Shales, and concealed 
 
 6. Sandstone, massive, and shales. 
 
 7. Coal i 
 
 Coal 
 
 0' 2" | 
 
 Shales 
 
 .... 2' 6" 1 
 
 Coal 
 
 ... 2' 4" ; 
 
 Shale 
 
 .... O' 6" i 
 
 Coal 
 
 .... 1' 8" I 
 
 Shales, sandstone, and concealed. 
 
 Shales 
 
 Coal, good 
 
 Shales, and concealed 
 
 Sandstone 
 
 Shale 
 
 Coal . 
 
 Coal <( Shale 
 
 Coal and slate. 
 
 Concealed, with shales, sandstones, and 
 two thin coals 
 
 ( Coal 2' 6" 
 
 < Shale; 5' 0" 
 
 ( Coal 6' 0" 
 
 Coal. Pocahontas 
 (No. Ill) 
 
 17. Shales, sandstone, and concealed 
 
 18. Coal (No. II) 
 
 19. Sandstone and shales 
 
 20. Coal (No. I) 
 
 21. Shales 
 
 22. Sandstone, gray 
 
 23. Shales, dark 
 
 24. Concealed 
 
 25. Sandstone, and concealed 
 
 26. Sandstone, gray, massive 
 
 27. Green, limy, fossiliferous shales, top of 
 
 Lower Carboniferous. 
 
 4001 
 
 1U0 | 
 
 35 
 20 f 
 
 60 I 
 
 95 J 
 
 110 / 
 
 55 
 
 100 ) 
 
 10 ? 
 
 3) 
 
 28) 
 35 
 20 ( 
 50 f 
 40 | 
 10 J 
 
 710 
 
 7 2 
 
 115 
 1 8 
 
 113 
 
 6 
 
 130 
 
 13 6 
 
 80 
 2 6 
 20 
 0 2 
 
 183 
 
 Total 1,402 
 
 The interval added to the top of the 
 Pottsville in this section is only an esti- 
 mate at best, and the amount may not 
 be near large enough, since the Ken- 
 tucky geologists report the series as 
 2,000 feet thick not many miles south- 
 west from this region. 
 
 The separate coal beds of this section 
 can not yet be satisfactorily correlated 
 with those on New River (Section 151); 
 At one time the writer was inclined to 
 believe that No. 7 might be the equiva- 
 lent of the Nuttall vein, and that No. 16 
 of this section was probably identical 
 with No. 18 of the Nuttallburg section 
 
WHITE.] 
 
 THE HOMEWOOD SANDSTONE. 
 
 199 
 
 (151), but the Pocahontas coal lies 200 feet nearer the base of the 
 Pottsville series than No. 18 does on New River, and hence unless this 
 part of the series thins away towards the southwest, which seems im- 
 probable, the possibility of identity is rather slender. The miuing 
 operations of the next few years, however, may be depended upon to 
 settle the question, since it has a more than scientific interest. 
 
 A cursory examination of the sections given will show that the 
 Pottsville series generally has something like the following structure : 
 
 Sandstone (Homewood). 
 
 Coal group (Mercer). 
 
 Sandstones (Counoquenessing). 
 
 Coal group (New River). 
 
 Sandstone (Sharon). 
 
 Of course when the series attains such an excessive thickness as on 
 the New River, for instance, the structure is more complicated than the 
 above scheme would indicate, and yet even then a general agreement 
 can usually be made out. 
 
 Having now glanced at the general structure of these measures, we 
 shall take up the more important members and describe them in detail. 
 
 CHARACTERISTIC HORIZONS. 
 
 THE HOMEWOOD SANDSTONE. 
 
 The Pottsville series is nearly everywhere capped with a coarse 
 sandstone, which is quite different in texture and general appearance 
 from any of the sandstones in the Coal Measures above. In the vicinity 
 of Homewood, Beaver County, Pennsylvania, this rock attains a thick- 
 ness of 150 feet, and was named from that locality. It is generally 
 quite massive, making great cliffs along the streams and covering the 
 summits with huge blocks arranged in “rock cities.” While usually 
 quite hard, it generally splits well and makes excellent building stone, 
 the blocks from it being almost indestructible. Although generally of 
 a yellowish or buffish gray tinge, it occasionally consists of almost pure 
 white quartz grains, and hence sometimes supplies glass sand of excel- 
 lent quality. This might be called the “ cascade” member of the Potts- 
 ville series, since it so often produces water-falls. 
 
 In Pennsylvania it is generally 30 to 50 feet thick, but occasionally, 
 as at Homewood and other points, it thickens up to 75 or even 150 feet. 
 
 Westward, in Ohio, the rock thins down and is often only 15 to 20 
 feet thick, but still distinctly recognizable as a heavy bedded, coarse 
 sandstone, filled with fossil stems and trunks of trees, mostly lepido- 
 dendron and sigillaria. It is seen in the bed of Little Beaver near its 
 mouth, and frequently between that point and Fredericktown. It is 
 the quarry rock in Coshocton County referred to in Vol. V (p. 104), Ohio 
 Geology, where it is 30 feet thick and of the same type so often found 
 in Pennsylvania. From this point on across Ohio, to Irouton and 
 
200 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65 . 
 
 Hanging Rock, it is frequently seen, and at the latter point makes one 
 of the great cliffs in the steep hillside which gave name to the place, 
 being there 40 feet thick. 
 
 Along the Great Kanawha this rock comes to water level at the 
 mouth of Armstrong Creek, and from there on up that stream, as well 
 as up the New and Gauley rivers, is a great cliff rock 150 to 200 feet 
 thick. It crowns the walls of the New River canon at Hawk’s Nest 
 and other points to Nuttallburg and beyond, where it seems to change 
 suddenly in character southward from that, becoming soft and easily 
 disintegrating to a heap of coarse, brown sand. 
 
 On the Tug fork of Big Sandy this stratum makes great cliffs along 
 the hills through the “roughs” of Tug, and sinks below that stream at 
 the mouth of Ben’s Creek, 95 miles above Louisa. 
 
 Ohio Pyle Falls, on the Youghiogheny River, is made by this rock, 
 and the upper portions of the great cascades on the Black Water and 
 Glady forks of Cheat pour over the same stratum. 
 
 It is the gas-bearing member in western Pennsylvania and northern 
 West Virginia. 
 
 THE MERCER GROUP. 
 
 In western Pennsylvania a group of coals associated with two fossil- 
 iferous limestones makes its appearance directly under the Homewood 
 sandstone, and extends almost uninterruptedly across the Ohio field to 
 Hanging Rock. It was first fully described from the vicinity of Mercer, 
 Pennsylvania, and named from that locality. When well developed 
 the group presents the succession seen in Section 140, and is 40 to 50 
 feet thick. 
 
 The two limestones are very much alike, except the Lower Mercer is 
 a little darker blue than the Upper, and is the more persistent. Both 
 are crowded with fossils and are frequently cherty, some of the famous 
 “ flint ledges ” of Ohio being made by one of these beds. Each lime- 
 stone usually carries an iron ore on its top of the variety known as 
 “block” ore. The Upper Mercer is known as the Zoar limestone in 
 many portions of Ohio, and its ore is called by several terms, among 
 which are u Dunkel Block,” “Franklin Block,” “Main Block,” “Big 
 Red Block,” etc. The Lower Mercer was formerly known as the “Blue' 
 limestone, and its corresponding ore as the “Blue Limestone Block,” 
 “ Little Block,” etc. 
 
 The Mercer coals are generally two, the upper one coming under the 
 Upper Mercer limestone and the lower one under the Lower Mercer 
 limestone. Occasionally there is also a coal on top of each limestone, 
 but these beds are sporadic, and hence do not merit a designation, 
 though Orton has applied the name “ Tionesta” to the Upper one in 
 Ohio, as the writer did in Report Q 2 , on Lawrence County, Pennsyl- 
 vania. 
 
 These Mercer coals are generally rich in ash, and are seldom mined 
 on a commercial scale, although they are quite persistent from western 
 
WHITE. | 
 
 THE CONNOQUENESSING SANDSTONES. 
 
 201 
 
 Pennsylvania all around the northern margin of the Ohio coal field. 
 Both of them occasionally become cannel in Ohio, the upper being the 
 Strawbridge cannel of Holmes County and the Bedford cannel of Co- 
 shocton, according to Orton, while the lower coal is the Flint Bidge 
 cannel of Licking County. Neither of these beds seldom exceeds 3 feet 
 in thickness, and they are more frequently only 1 or 2. 
 
 Eastward from Mercer and Lawrence Counties, Pennsylvania, the 
 limestones disappear from this group and the coals thin away, except 
 around the northern rim of the coal field, where, in McKean County, 
 the Alton coal group of Ashburner probably represents the Mercer 
 coals, so that usually only one is left, and it is generally quite impure. 
 This bed has received a different name for nearly every locality where 
 it attains workable thickness. Bogers called it the Tionesta coal in 
 Forest County, Pennsylvania, and it is the Mount Savage bed of Som- 
 erset. Along the north Potomac Biver it frequently appears in the 
 cuts of the West Virginia Central Bailroad, and is there known as the 
 “Bailroad seam.” It has been mined for local use just above Valley- 
 Falls, Taylor County, West Virginia, where it lies near water level, 
 and is 4 feet thick, with a slate near center. It always presents a coarse 
 structure, and no first-class fuel is ever obtained at this horizon. Along 
 the New Biver, and through ail the country between it and the Tug 
 Fork, only an insignificant coal, 1 to 2 feet thick, occurs at this level. 
 
 The famous Mount Savage fire clay of Pennsylvania and Maryland 
 comes within the limits of the Mercer group, and directly underlies the 
 Mount Savage coal, which it occasionally replaces. 
 
 THE CONNOQUENESSING SANDSTONES. 
 
 Below the Mercer group- there comes the great sandstone horizon 
 par excellence of the Pottsville series. This group is generally triple, 
 there being a massive sandstone at top, then a coal and shale interval, 
 below which is another massive sandstone. These sandstones were 
 first studied by the writer along the Oonnoquenessiug Biver, in Law- 
 rence County, Pennsylvania, and they were designated from that 
 stream. The Massillon sandstone of Newberry represents only a por- 
 tion of the group; otherwise it would have precedence in nomenclature. 
 
 Each of these sandstone members is from 40 to 50 feet thick, though 
 occasionally the shale and coal separating them thins out and they 
 coalesce into one mass 150 to 200 feet thick, or even more. They are 
 generally quite hard, the quartz grains being finer and more compactly 
 arranged than in the Homewood sandstone above. The color is more 
 frequently yellowish white than any other, though sometimes it is gray. 
 
 The Quakertown coal comes between the two sandstone members of 
 the group. It seldom exceeds 2 feet in western Pennsylvania or east- 
 ern Ohio, and unless it should be the “ Jackson shaft,” or u Wellstou” 
 coal, it does not seem to attain much importance in that State, though 
 it is often present in the series as a thin bed, being represented in the 
 
202 THE NORTHERN BITUMINOUS COAL FIELD. [bull. 65 . 
 
 Hanging Rock section (147) by number 13, which is only 2 feet thick, 
 slate and all. . 
 
 East from the Mahoning River no workable coal is known at this 
 horizon in Pennsylvania, though a thin coal or black slate is often 
 present. 
 
 THE NEW RIVER COAL GROUP. 
 
 The great development of coal in the middle and lower half of the 
 Pottsville series along New River, West Virginia, has given name to 
 this group. Although there are thin representatives of the group in 
 nearly every section of the Pottsville which is exposed in Pennsylvania, 
 yet only around the northwestern margin of the field in that State is 
 any valuable coal found at this horizon, namely, the Sharon coal of 
 Mercer County. This bed occurs in pockets and isolated basins, in the 
 western part of Mercer, where it is 3 to 5 feet thick, and a “ block,” or 
 open-burning coal of great purity. It enters Ohio in the same patchy 
 condition, and extends through Mahoning, Trumbull, Portage, Summit, 
 Stark, Medina, and Wayne Counties of northeastern Ohio, and it is 
 probably the “Jackson shaft” or “ Wellston” seam of Jackson County 
 in southern Ohio. In all cases it is the same open-burning, pure fuel, 
 very low in ash and sulphur. 
 
 This Sharon bed and its thin rider appear to represent all the coals 
 iu the New River group, and hence it can not be called identical with 
 any one of them, though according to Prof. Fontaine the flora of the 
 Sharon roof shales is very similar to that found in the roof of the 
 Quinnimont bed on New River. These roof shales of the Sharon coal 
 through western Pennsylvania and across Ohio are a very character- 
 istic feature. They begin directly under the Connoquenessing sand- 
 stones, and are often 40 to 50 feet thick; of a dark blue color, and 
 generally contain much iron ore (carbonate) in nuggets and bands. 
 These shales show the same character at Hanging Rock (Section 147), 
 in southern Ohio, as they do on the Mahoning at the east. 
 
 In passing southward from Pennsylvania, along the Alleghany Moun- 
 tain region, one of these New River beds thickens up to 3 feet in Garrett 
 County, Maryland, just east from the West Virginia line, and has there 
 been mined for local use on the land of Mr. Browning. It comes near 
 the base of the Pottsville series, is quite soft and pure, and exhibits the 
 same coking type as these coals all do on New River. One of these 
 beds is also workable along Shaver’s Fork of Cheat River, east from 
 the Beverly Valley. This coal group, which is well shown in the Black 
 Water section (133) of Tucker County, grows in importance southwest- 
 ward through Randolph, Webster, Greenbrier and Nicholas Counties, 
 into Fayette, where at Nuttallburg on New River we find the type 
 section of the group (No. 151), which there incloses three workable coal 
 beds besides several too thin to be of economic importance. The three 
 workable beds are, in descending order, the Nuttall, Fire Creek, and 
 Quinnimont, with the intervals separating them shown in Section 151. 
 
THE POTTSVILLE CONGLOMERATE CLIFFS AND DEBRIS ON NEW RIVER, WEST VIRGINIA, NEAR FAYETTE. 
 
THE LIBRARY 
 OF THE 
 
 UNIVERSITY OF ILLINOIS 
 
WHITE.] 
 
 THE NEW RIVER COAL GROUP. 
 
 203 
 
 These coals vary from 3 to 5 feet in thickness along New River, and 
 are the ones from which the celebrated New River coke is now manu- 
 factured. The Nut tall is the most regular and persistent, being th£ 
 only one which dips below water level at the north with a workable 
 thickness. 
 
 They are all quite soft, very low in ash and sulphur, and rich in fixed 
 carbon, making coke of the greatest purity. 
 
 The Fire Creek and Quinnimont beds are quite irregular in their dis- 
 tribution and thickness, but both of them furnish much good coal on 
 New River. I have termed the lowest bed the Quinnimont, but the 
 stratigraphical horizon of the Quiunimont seam is not yet settled- since 
 it may prove identical with the Fire Creek bed, but all the coal oper- 
 ators agree that there are three workable coals on New River, and that 
 Nos. 11, 16, and 18 of Section 151 are these three beds, whatever their 
 identity with reference to the Fire Creek and Quinnimont localities 
 may be. 
 
 South westward from Fayette County towards Raleigh, Mercer, and 
 McDowell, the New River coals still continue to increase in thickness 
 and importance, culminating in the great bed at Pocahontas, in the edge 
 of Virginia. 
 
 Section on Crane Creek , West Virginia , near Pocahontas , Virginia . — 
 Section 152 shows the succession of these coals on Crane Creek, a trib- 
 utary of Blue Stone, a few miles northeast from Pocahontas. Here 
 the Pocahontas coal is divided into two benches by a layer of shale 5 
 feet thick, but at Pocahontas it exhibits the following structure: 
 
 Ft. in. 
 
 Coal 9 6 ] Ft. in. 
 
 Shale 0 4 )> g 
 
 Coal 0 10 j 
 
 There is a bony streak about 2 feet below the top of the coal, but it 
 is not rejected in mining. 
 
 Section at head of South Elk Horn Creek , McDowell County, West Vir- 
 ginia. — Across the Flat Top Mountain divide from Pocahontas, around 
 the head of South Elk Horn Creek, in McDowell County, this coal ex- 
 hibits the following structure: 
 
 Ft. in. 
 
 Coal 3 8 ') 
 
 Bony coal 0 8 I Ft. 
 
 Coal 2 3 )> 9 
 
 Coal 2 4 J 
 
 Section on East Branch of Simmons Creek , Mercer County, West Vir- 
 ginia. — On the east branch of Simmons Creek this coal shows as follows: 
 
 Coal 
 
 Slate, blue 
 Coal 
 
 Ft. 
 
 2 
 
 0 
 
 0 
 
 in. 
 
 2 ) Ft. in. 
 
 4 ) 8 10 
 
204 
 
 THE NORTHERN BITUMINOUS COAL FIELD. 
 
 [BULL. 65 . 
 
 Section on west branch of Flipping Creelc , Mercer County , WestVirginia . — 
 On the Walker tract, west branch of Flipping Creek, the coal has this 
 structure : 
 
 Ft. in. 
 
 Coal 
 
 Dark shales 
 Coal 
 
 2 
 
 10 
 
 6 
 
 6 
 
 0 
 
 0 
 
 ) Ft. in. 
 >18 6 
 
 Section on Pinnacle Fork of the Guyandotte River, Wyoming County , 
 West Virginia. — Just before this coal passes under the level of the 
 Pinnacle Fork of the Guyandotte Eiver west from Flat Top Mountain 
 it exhibits the following structure : 
 
 Ft. in. 
 
 Massive sandstone 
 
 Coal 
 
 Fire clay 
 
 Sandy shale 
 
 Coal 
 
 1 
 
 3 
 
 5 
 
 5 
 
 4 
 
 0 
 
 0 
 
 4 
 
 Ft. in. 
 14 8 
 
 This coal was numbered III in the original section published from 
 Pocahontas by Maj. Jed. Hotchkiss, and it is frequently known by that 
 name. Major Hotchkiss thinks the Pocahontas bed identical with the 
 Quinnimont of New Kiver, but the writer can not yet satisfactorily cor- 
 relate this bed with any of the New River coals which have been mined. 
 
 The coal from the Pocahontas seam is quite as pure and valuable for 
 coke and general fuel purposes as any in the New River field, and, in 
 fact, is the same kind of coal. 
 
 Two other beds of 4 to 5 feet in thickness occur in the hills above the 
 Pocahontas vein, but so far they have not been mined to any extent, as 
 they are not regular in thickness and the great bed below monopolizes 
 the present mining operations. 
 
 THE SHARON CONGLOMERATE. 
 
 The interval below the Sharon coal in Ohio and western Pennsylvania 
 down to the base of the Pottsville series is often occupied by a mass- 
 ive conglomerate, and when it is absent the coal with its under-clay 
 rests directly on the Lower Carboniferous beds. This conglomerate 
 stratum was considered a separate member of the series by the Ohio 
 geologists and as representing the entire No. XII conglomerate of Rog- 
 ers in Pennsylvania. 
 
 But later studies have shown that it is simply the basal member of 
 this series. When well developed in Ohio it is very coarse, being a 
 mere mass of pebbles from a pea to an egg in size. There is no single 
 stratum around the southeastern margin of the Appalachian field that 
 will exactly compare with the Sharon conglomerate in physical aspect, 
 though local streaks in all these great sandstones are quite as pebbly, 
 but just as the Sharon coal is represented by several beds in the New 
 River section, so the Sharon conglomerate, only 20 to 40 feet thick in 
 
WHITE.] 
 
 THE LOWER CARBONIFEROUS. 
 
 205 
 
 Pennsylvania and Ohio, is on New Biver represented by 300 to 400 feet 
 of shales, sandstones, and conglomerates. 
 
 In northern Pennsylvania the Olean con glomerate of Bradford County 
 and the Garland conglomerate of Warren have been shown by Mr. John 
 F. Carll to be identical with the Sharon stratum, and they also resemble 
 it very much in physical characters. The coarse type of the Sharon 
 conglomerate appears to be confined to the northwestern rim of the 
 Appalachian field, since it disappears southward under the other mem- 
 bers of the series. 
 
 the lower carboniferous beds. 
 
 Below the base of the Pottsville series come the red shales and lime- 
 stones of the Mauch Chunk series, and then succeed the gray sandstones 
 of the Pocono, the lowest series of the Carboniferous system. 
 
 Thin coals occur locally in both of these members of the Lower Car- 
 boniferous in Pennsylvania and West Virginia, but nowhere in these 
 States, nor in Ohio, does any merchantable bituminous coal exist in 
 this portion of the Carboniferous. 
 
 The Tipton Bun coals of Blair County, Pennsylvania, have been cited 
 as occurring in the Pocono sandstone series for the last thirty-five years, 
 and this conclusion is reiterated by Mr. Ashburner in a special report 
 made as late as 1885 (Pennsylvania Geological Survey, Annual Beport, 
 1885, p. 250), but a single glance at the fossil plants occurring in the 
 roof shales of the coals now mined there proves that they belong to the 
 Lower Coal Measures, or Alleghany Biver series, and not to the Pocono, 
 their apparent stratigraphical position being the result of displacement, 
 so that although the Pocono series is reported to contain valuable coal 
 beds in Montgomery County, Virginia, it certainly does not in any of 
 the three States covered by this report, and hence a further consider- 
 ation of the Lower Carboniferous beds is not germane to this publica- 
 tion. 
 
INDEX. 
 
 A. 
 
 Page. 
 
 Aleppo Township, Greene County, Penn- 
 sylvania, section in — 24 
 
 Alleghany County, Maryland, section 
 
 in 56 
 
 Alleghany County, Pennsylvania, sections 
 
 in 73,112 
 
 Alleghany River series 99-178 
 
 table showing strata of 101 
 
 Alton coal group = Mercer coals 201 
 
 Ames limestone 90-91 
 
 Andrews, E. B., section given by 28 
 
 Antiquity, Ohio, section at 53 
 
 Arbuckle, West Virginia, section at 54 
 
 Armstrong County, Pennsylvania, sec- 
 tions in 107, 108, 109, 110, 111, 184 
 
 Armstrong Creek, West Virginia, section 
 
 at mouth of 140 
 
 Arno coal 167 
 
 Ashlmnier, C. A., sections given by 104, 182 
 
 geologi c identifications by 174 
 
 Athens County, Ohio, sections in 66, 133, 134 
 
 B. 
 
 Baird Ore, Ohio 173 
 
 Bakerstown coal 92-93 
 
 Baltimore and Ohio Railroad, section on. . 188 
 
 Barbour County, West Virginia, sections 
 
 in 128,161 
 
 Barclay, Mr., section furnished by 190 
 
 Baresville, Ohio, section at 28 
 
 Barnet coal= Middle Kittanning coal 166 
 
 Barren Measures or Elk River series ... 19, 70-98 
 Beaver County, Pennsylvania, section in. 112 
 Beaver River, Pennsylvania, section near 
 
 mouth of 172 
 
 Beaver Run, Pennsylvania, section on... 114 
 
 Bedford County, Pennsylvania, sections 
 
 in 77,149 
 
 Bellaire, Ohio, section at 68 
 
 section near 50 
 
 Bellton, West Virginia, section at 26 
 
 Bellton coal group 32, 34 
 
 Belmont County, Ohio, sections in 50, 67, 68 
 
 Bennington, Pennsylvania, section at 122 
 
 Ben's Creek, Cambria County, Pennsylva- 
 nia, section at 120 
 
 Berlin, Pennsylvania, section at 76 
 
 Berry’s Mine, Morgan County, Ohio, sec- 
 tion at 67 
 
 Big Hurricane Creek, Putnam County, 
 
 West Virginia, section at 55 
 
 Tfege. 
 
 Big Sandy River, Lawrence County, Ken- 
 tucky, section on 194 
 
 Black Fossiliferous limestone 93 
 
 Blacksville limestone 36 
 
 Blaine Creek, Lawrence County, Ken- 
 tucky, section at mouth oi 144 
 
 section on 162-163 
 
 Blair County, Pennsylvania, section in... 122 
 
 Blossburg, Pennsylvania, section at 102 
 
 Bloss vein, Pennsylvania= Lower T 4ittan- 
 
 ning c^al 169 
 
 Board Tree Tunnel, Marshall County, 
 
 West Virginia, section at 25 
 
 Bolivar fire clay 159-160 
 
 Bolivar, Pennsylvania, section near 115 
 
 Booth’s Creek, West Virginia, section on. 189 
 
 Brady Township, Butler County, Pennsyl- 
 vania, section at 107 
 
 Broad Top, Pennsylvania, section at 76-77 
 
 Broad Top Basin, Huntingdon County, 
 
 Pennsylvania, sections in 125, 126, 185 
 
 Brockway ville, Pennsylvania, section near 104 
 
 Brooke County, West Virginia, section in 190 
 
 Brookville, Pennsylvania, section at 183 
 
 Brookville coal=Clarion coal in Ohio .... 175 
 
 Brookville coal 178 
 
 Brown, C. N., sections furnished by 50, 67, 68 
 
 Brown’s Mills, Monongalia County, West 
 
 Virginia, section near 38 
 
 Brownstown, West Virginia, section near 189 
 
 Brownsville, Pennsylvania, section at 44 
 
 Brownsville coal=Washington coal 37 
 
 Browntown sandstone 58 
 
 Brush Creek coal = Masontown coal 94, 96 
 
 Brush Creek coal = Mahoning coal 96 
 
 Brush Creek limestone = Lower Cam- 
 bridge limestone 93 
 
 Bryan’s Bank, Upshur County, West Vir- 
 ginia, section at 152 
 
 Buckbannon River, West Virginia, section 
 
 on 152 
 
 Bnchtel limestone = Upper Freeport 159 
 
 , Bnchtel, Ohio, section near 133 
 
 Buffalo Creek, Marion county, West Vir- 
 ginia, section at 48 
 
 Buhrstone iron ore 173 
 
 Burning Spring, Kanawha County, West 
 
 Virginia, natural gas first used at. 196 
 
 section at 196 
 
 Burning Springs, Wirt County, West Vir- 
 ginia, sections at 52, 83 
 
 section near 192 
 
 Butler County, Pennsylvania, section in . . 107 
 
 207 
 
208 
 
 INDEX. 
 
 Cabell County, West Virginia, sections 
 
 in . .,..66, 
 
 Cambridge limestones 
 
 Cambria County, Pennsylvania, sections 
 
 in .118, 119, 120, 122, 
 
 Campbell’s Creek coal vein 
 
 Campbell’s Creek limestone 
 
 Camp Branch, Cabell County, West Vir- 
 ginia, section near 
 
 Cannelton coals 
 
 Cannonsburg, Pennsylvania, section at.. . 
 Carboniferous System, Rogers’s table 
 
 showing subdivisions 
 
 Carll, John F., geologic identifications by. 
 Carpenter’s station, Pennsylvania, section 
 
 near 
 
 Cassville plant shale 
 
 Cedar Grove coal 
 
 Centreville, Pennsylvania, section near... 
 Chance, H. Martyn, sections given by . . . 
 
 107, 
 
 cited on geologic equivalent of Upper 
 
 Kittanning in Pennsylvania 
 
 geologic identifications by 
 
 Chapline Hill, Wheeling, West Virginia, 
 
 section at 
 
 Charleston, West Virginia, section near. . . 
 
 sections at 
 
 Cheat River, Tucker County, West Vir- 
 ginia, sections on 
 
 Clarion coal 
 
 Clarion County, Pennsylvania, sections 
 
 Page. 
 
 155, 158 
 93 
 
 148, 149 
 170 
 168 
 
 155 
 
 97 
 
 78 
 
 19 
 
 205 
 
 113 
 41 
 167 
 108 
 105, 106, 
 123, 183 
 
 165 
 175, 178 
 
 85 
 
 136, 195 
 
 187, 188 
 175-176 
 
 in 105, 106, 183 
 
 Clarion sandstone 176 
 
 Clarksburg limestone 88 
 
 Clarksburg, West Virginia, sections at.. 48-49, 129, 
 
 189 
 
 coal bed at 88 
 
 Clearfield County, Pennsylvania, sections 
 
 in 103, 124, 182 
 
 Clearfield, Pennsylvania, sections at. . .123, 182-183 
 Clinton coal = Middle Kittanning coal... 166 
 Coalburg, West Virginia, coal beds at ... . 96 
 
 section at 162 
 
 Coal Valley gas vein, West Virginia 170 
 
 Cole, R. A., sections given by 130, 192 
 
 Columbia mine, Westmoreland County, 
 
 Pennsylvania, section at 68 
 
 Coleman limestone 93 
 
 Columbiana County, Ohio, section in 131 
 
 Colvin’s Run, Greene County, Pennsylva- 
 nia, section on 23 
 
 Colvin’s Run limestone 89 
 
 Conemaugh, Pennsylvania, section at ... . 119 
 
 Connellsville sandstone 87 
 
 Conoquenessing sandstones 201 
 
 Cook vein, West Virginia 171 
 
 Copeman’s Knob, West Virginia, section 
 
 at 65 
 
 Cove Creek, Wayne County, West Vir- 
 ginia, sections on 155-156, 157 
 
 Craig, Geo., record of boring furnished 
 
 by 54 
 
 Crane Creek, Mercer County, West Vir- 
 ginia, sections on 198, 203 
 
 Page. 
 
 Cressov, Pennsylvania, section at 122 
 
 Crinoidal coal 91,92 
 
 Crinoidal limestone 90-91 
 
 Cucumber Run, Fayette County, Pennsyl- 
 vania, section on 116 
 
 Current’s farm, Upshur County, West 
 
 Virginia, section at 152 
 
 D. 
 
 Dickinson Salt Works, West Virginia, 
 
 section at 138 
 
 Doubleday, Mr., section furnished by 114 
 
 Dunbar Creek, Fayette County, Pennsyl- 
 vania, section at 74 
 
 Dunkard coal 33-34 
 
 Dunkard Creek beds, fossils of 41-42 
 
 Dunkard Creek, Greene County, Pennsyl- 
 vania, section on 22 
 
 Dunkard Creek series 19, 20^42 
 
 highest beds of 30 
 
 age of 41-42 
 
 Dunkard Creek series. See Permo-Car- 
 boniferous. 
 
 E. 
 
 Eagle limestone 141, 177 
 
 Eagle, West Virginia, section at 176 
 
 East Brady, Pennsylvania, section at 106 
 
 Edwards, W. S., sections furnished by... 136,195 
 
 Elk County, Pennsylvania, sections in .. 104, 182 
 
 Elk Lick coal *. 89-90 
 
 Elk Lick limestone 90 
 
 Elk River series 70-98 
 
 Elk River, West Virginia, section at 
 
 mouth of - 136 
 
 Epler oil boring, Washington County, 
 
 Ohio, section at 192 
 
 F. 
 
 Fairfax, Knob, West Virginia, section at. 65 
 
 section near 82 
 
 Fall Brook, Pennsylvania, section at 103 
 
 Farmington, West Virginia, section at... 37 
 
 section near 189 
 
 Fayette County, Pennsylvania, sections 
 
 in 44,74,116 
 
 Fayette County, West Virginia 176, 197 
 
 Federal Creek, Ohio, section at 67 
 
 Ferriferous limestone 173-175 
 
 Fire Creek coal - 203 
 
 Fish Creek sandstone 33 
 
 Fishing Creek, Wetzel County, West 
 
 Virginia, section on 38 
 
 Fishpot limestone = Sewickley limestone. 62 
 Fleming, Cochran, records of borings fur- 
 nished by 73, 112 
 
 Flipping Creek, West Virginia, section on 204 
 
 Fontaine, W. M., formation named by 179 
 
 Fossil horizons and localities 31, 34, 35, 37; 38, 
 
 41, 42, 57, 59, 60, 62, 79, 90-91, 94, 
 97, 98, 159, 163, 169, 177, 179-180 
 Fossils of the Upper Coal Measures 69 
 
 Fossil plant horizons and localities . - 34, 35, 37, 38, 
 
 41, 42, 57, 97, 169, 179-180, 205 
 
INDEX. 
 
 209 
 
 Page. 
 
 Fox Township, Elk County, Pennsylva- 
 nia, section in 182 
 
 Freeport coals 160-161 
 
 Freeport limestone 163 
 
 Freeport, Pennsylvania, section at Ill 
 
 Freeport sandstone 163-164 
 
 Fulton, John, sections given by 118, 122 
 
 Fulton vein, Pennsylvania = Lower Kit- 
 
 tanningcoal 169 
 
 G. 
 
 Gallitzin coal=Mahoning coal (?) 96 
 
 Gallitzin, Pennsylvania, sections near 148-149 
 
 Gas (natural) first used for manufacturing 
 purposes at Burning Spring, "West 
 
 Virginia 196 
 
 Gilboy sandstone =Browntown sandstone 58 
 
 Gilmer County, "West Virginia, section in. 53 
 
 Gilmore sandstone 31 
 
 Gladden’s Run, Pennsylvania, section on. 186 
 
 Gray Ore, Ohio 173 
 
 “Great” Conglomerate =Pottsville Con- 
 glomerate 179 
 
 “ Great ” limestone 59-60 
 
 Greene County, Pennsylvania, sections 
 
 in 22,23,24,45 
 
 Green Fossiliferous limestone 90-91 
 
 Guernsey County, Ohio, section in 83 
 
 Guyandotte Mountain, West Virginia, sec- 
 tion at 142 
 
 Guyandotte River, West Virginia, sec- 
 tions on - 155,204 
 
 H. 
 
 Hacker’s Valley post-office, West Vir- 
 ginia, section at 153 
 
 Haggerty, John, sections furnished by . . . 105-106 
 
 Hanging Rock, Ohio, section at 193 
 
 Harrison County, Ohio, section in 68 
 
 Harrison County, West Virginia, sections 
 
 in 48,49, 129,189 
 
 Hartford City, W est Virginia, section at . . 53-54 
 
 Hartley’s bank, near Masontown, West 
 
 Virginia, section at 150 
 
 Hobson coal = Washington coal 37 
 
 Hocking Valley, Ohio, sections in 133, 168 
 
 Hog Hollow coal = Middle Kittanning 
 
 coal , 166 
 
 Holly River, West Virginia, section on. .. 153 
 
 Holmes County, Ohio, section in 191 
 
 Homewood sandstone 199 
 
 Horton Township, Elk County, Pennsyl- 
 vania, section at 104 
 
 Hostetter coal _ 33 
 
 Hotchkiss, Jed, section given by 204 
 
 Houtzdale, Pennsylvania, section near. . . 124 
 
 Hukill, E. M., section furnished by 113 
 
 Huntingdon County, Pennsylvania, sec- 
 tions in 125, 185 
 
 Huntington, West Virginia, sections at . . 66, 84 
 
 section near 158 
 
 L 
 
 Indiana County, Pennsylvania, sections in 115 
 
 Irondale limestone and ore 95 
 
 Bull. 65 14 
 
 Page. 
 
 Iron ore in the Upper Coal Measures 57-58 
 
 Ironton, Ohio, sections near 135 
 
 J. 
 
 Jackson County, Ohio, section in 193 
 
 Jackson Furnace, Jackson County, Ohio, 
 
 section near 193 
 
 Jackson, T. M., sections furnished by 129, 189 
 
 Jackson Township, Cambria County, 
 
 Penn syl vania, section in 119 
 
 Jefferson County, Ohio, section in 68 
 
 Jefferson County, Pennsylvania, section 
 
 in 183 
 
 Johnston, John L., section furnished by . . 49 
 
 Johnstown (Cement) limestone 165-166 
 
 Johnstown, Pennsylvania, section at 118 
 
 Jolly town coal 34 
 
 Jollytown limestone 34 
 
 Jordan, Col., record of boring near Charles- 
 ton, West Virginia, furnished by . . 137 
 
 K. 
 
 Kanawha Black Flint 98 
 
 Kanawha County, West Virginia, sections 
 
 in 85,136,138,162,195,196 
 
 Karthaus, Pennsylvania, section near 103 
 
 Kellersburgh, Pennsylvania, section at... 184 
 
 Kenova, West Virginia, section near 158 
 
 Kittanning coals 164-165, 166-167, 169-170 
 
 Kittanning fire clay 171 
 
 Kittannin g, Pennsylvania, section near. . . 109 
 
 Kittanning sandstone 172 
 
 L. 
 
 Laughlintown, Pennsylvania, section near 116 
 
 Laurel Run, Westmoreland County, Penn- 
 sylvania, section on 116 
 
 Lawrence County, Kentucky, sections in 144, 145 
 
 162-163, 194 
 
 Leading Creek, Gilmer County, West Vir- 
 ginia, section on 53 
 
 Letonia, Ohio, section near 132 
 
 Lesley, J. P., Pottsville conglomerate 
 
 named by 179 
 
 Lewis County, West Virginia, section in . 153 
 
 Liberty Township, Washington County, 
 
 Ohio, section at 29 
 
 Lick Run, West Virginia, section at mouth 
 
 of 137 
 
 Ligonier, Pennsylvania, section at 75 
 
 Limestone Hill, West Virginia, exposure 
 
 of limestone at 33 
 
 Limestone ore, Ohio 173 
 
 Linton, Prof., sections given by 113,185 
 
 Little Beaver Creek, Pennsylvania, sec- 
 tion at mouth of 130 
 
 Little Clarksburgh coal 88 
 
 Little Falls, West Virginia, section at 80 
 
 Little Kanawha River, West Virginia, 
 
 section on 153 
 
 Little Laurel Creek, West Virginia, sec- 
 tion on 156 
 
 Little Pittsburgh coal 88-87 
 
210 
 
 INDEX, 
 
 Page. 
 
 Little ‘Washington coal 39 
 
 Little Waynesburg coal 58 
 
 Lloyd Wamsley’s bank, Upshur County, 
 
 West Virginia, section at 152 
 
 Lockport, Pennsylvania, section near 115 
 
 Logansport, Pennsylvania, section at 110 
 
 Logan County, West Virginia, section in. 147 
 Lovejoy, E., sections in Ohio furnished by . 66, 67 
 
 Lower C am bridge limestone =Bru sh C reek 
 
 limestone 93 
 
 Lower Cambridge limestone=Philson 
 
 limestone 94 
 
 Lower Carboniferous beds 205 
 
 Lower Coal Measures 19, 99-178 
 
 Lower Coal Measures, table showing strata 
 
 of 101 
 
 Lower Freeport coal 160-161 
 
 Lower Freeport limestone 163 
 
 Lower Freeport sandstone 163-164 
 
 Lower Kittanning coal 169-170 
 
 M. 
 
 Mahoning coal 96 
 
 Mahoning County, Ohio, section in 191 
 
 Mahoning limestone 96-97 
 
 Mahoning River, Ohio, section on 191 
 
 Mahoning sandstones 95-96, 97 
 
 Malden, West Virginia, section near 138 
 
 Maple Swamp water tank, West Virginia 
 
 Central R. R., section at 127 
 
 Mapletown coal = Sewickley coal 61 
 
 Marietta sandstones 35-36 
 
 Marion County, West Virginia, sections 
 
 in 37,48,129,189 
 
 Marshall County, West Virginia, sections 
 
 in 25, 26 
 
 Martin County, Kentucky, section in 146 
 
 Mason County, West Virginia, sections in. 54 
 
 Masontown, West Virginia, coal bed at.. 94 
 
 Masontown, West Virginia, section near. 150 
 
 Massillon sandstone = Connoquenessing 
 
 sandstones in part 201 
 
 Mauch Chunk red shale, geologic place of. 19 
 
 McCoy shaft, near Gallitzin, Cambria 
 
 County, Pennsylvania, section at. 148-149 
 
 McCuneville, Ohio, section near 133 
 
 McDowell County, WestVirginia, section 
 
 in 203 
 
 Meeker’s Run, Athens County, Ohio, sec- 
 tion on 134 
 
 Mehaffey, J. A., section on Beaver Run, 
 
 Pennsylvania, given by 114 
 
 Meigs County, Ohio, sections in 63, 66 
 
 Meigs Creek coal = Sewickley coal 61 
 
 Mercer County, Pennsylvania, sections in . 190 
 
 Mercer County, West Virginia, sections 
 
 in 198, 203, 204 
 
 Mercer group 200-201 
 
 Middle Cannelton coal 97 
 
 Middle Freeport coal 160 
 
 Middle Kittanning coal 166-167 
 
 Miller’s Eddy, Pennsylvania, section at.. 105 
 
 Mineral County, West Virginia, sections 
 
 in 126, 127, 186 
 
 Minshall, F, W., sections furnished by. . 29, 
 
 52, 83, 192 
 
 Page. 
 
 Moatsville, Barbour County, West Vir- 
 ginia, section at 128 
 
 Monongalia County, West Virginia, sec- 
 tions in 38, 46, 47, 79, 80 
 
 Monongahela River series 42-69 
 
 Morgantown sandstone 88-89 
 
 Morgantown, West Virginia, section at . . 79 
 
 Morrisdale, Pennsylvania, section near.. 123 
 Moundsville, West Virginia, section at. . . 51 
 
 Mountain limestone, geologic place of 19 
 
 Mount Equity mine, Bedford County, 
 
 Pennsylvania 149 
 
 Mount Morris limestone 39-40 
 
 Mount Vernon furnace, Ohio, section near 134 
 
 Mumble-the-Peg Creek, Nicholas County, 
 
 West Virginia, section on 154 
 
 Murray sville, Pennsylvania, sections 
 
 at 114, 184-185 
 
 Muskingum County, Ohio, section in 132 
 
 N. 
 
 Natural gas first used for manufacturing 
 purposes at Burning Spring, West 
 
 Virginia 196 
 
 Nelson ville, Ohio, section near 134 
 
 New Bethlehem, Pennsylvania, section at. 106 
 
 Newburg, West Virginia, sections at 65, 81, 
 
 117, 167, 170 
 
 New Lisbon, Ohio, section near 132 
 
 New Martinsville, West Virginia, section 
 
 at 27 
 
 New River coal group 202-203 
 
 New Straitsville, Ohio, section at 168 
 
 Nicholas County, West Virginia, sections 
 
 in 153,154 
 
 Nineveh coal 32 
 
 Nineveh limestone - 32-33 
 
 Nineveh sandstone 32 
 
 Nuttallburg, West Virginia, section at. .. 197 
 
 Nuzum’s Mill, Marion County, West Vir- 
 ginia, section at 129 
 
 O. 
 
 Oceana, West Virginia, section at 143 
 
 Ohio County, W est Virginia, sections in . . 49, 130 
 
 Ohio Geological Survey reports cited 28, 66, 
 
 67, 68, 132, 134, 135, 161, 165, 168, 178, 191, 199 
 Old Peach Orchard, Lawrence County, 
 
 Kentucky, section at 145 
 
 Oliphant, F. H., record of borings given 
 
 by '....144,145,194 
 
 Ore Hill furnace, section near 107 
 
 Orton, Edward, strata named by * 93 
 
 beds of lower coal measures traced 
 
 across Ohio by 101 
 
 cited on subdivision of Ferriferous 
 
 limestone in Ohio 131 
 
 sections given by 134, 135 
 
 cited on Ohio equivalent of Upper 
 
 Kittaning 165 
 
 cited on Ohio coal beds 158 
 
 cited on geologic equivalent of Upper 
 
 Kittanning in Ohio 165 
 
 cited on Middle Kittanning coal in 
 
 Ohio 167 
 
 geologic identifications by 175 
 
INDEX. 
 
 211 
 
 P. 
 
 Page. 
 
 Panther Hill, Ohio, section at 134 
 
 Parkersburg, West Virginia, sections at. . 130, 192 
 
 Parsons, James, section furnished by 187 
 
 Patton station. Clarion County, Pennsyl- 
 vania ,. 183 
 
 Peach Orchard coal, geologic place of 146 
 
 Pennsylvania Geological Survey reports 
 
 cited. 29, 31, 37, 42, 44, 68, 74, 93, 94, 103, 104, 
 105, 106, 107, 108, 116, 120, 121, 122, 123, 125, 
 126, 149, 169, 173,182,183, 184, 185, 189, 190,205 
 
 Permo-Carboniferous or Dunkard Creek 
 
 series 19, 20-42 
 
 age of 41-42 
 
 Perry County, Ohio, sections in 133, 168 
 
 Philippi, West Virginia, section at 161 
 
 Philson limestone = Lower Cambridge 
 
 limestone 94 
 
 Piedmont, West Virginia, sections at 126, 186 
 
 Pine Creek limestone 93 
 
 Pinkerton Point, Pennsylvania, section at 121 
 Pipe Creek, Belmont County, Ohio, sec- 
 tion at 51 
 
 Pittsburgh coal 63-64 
 
 Pittsburgh coal iron ores 86 
 
 Pittsburgh limestones 87 
 
 Pittsburgh, Pennsylvania, section at 184 
 
 Pittsburgh region, section in 72 
 
 Pittsburgh sandstone 63 
 
 Plant horizons and localities, 34, 35, 37, 38, 41, 42, 
 57, 97, 169, 179-180, 205 
 
 Platt, Franklin, strata named by 90 
 
 geologic identifications by 91 
 
 sections given by 103, 120, 121, 122 
 
 Platt, Messrs., strata named by 63 
 
 section furnished by 76 
 
 geologic identifications by 89, 164 
 
 cited on geologic place of Johnstown 
 
 Cement limestone 166 
 
 Platt, Wm. G., sections given by.. 104, 108, 115, 184 
 Pocahontas, West Virginia, section near. 203 
 
 Pocono sandstone, geologic place of 19 
 
 Pomeroy, Meigs County, Ohio, section at 66 
 Porter’s (Greene), Twelve Pole Creek, 
 
 West Virginia, section at 158 
 
 Posten’s bank, near Mason town, West 
 
 Virginia, section near 150 
 
 Pottsville Conglomerate series 19, 179-205 
 
 Pottsville series, structure of 199 
 
 Powell Mountain, West Virginia, section 
 
 at....: 153 
 
 Preston County, West Virginia, sections in 65 
 117, 150, 167, 170, 188 
 Putnam County, West Virginia, sections in 55, 56 
 Putneyville, Pennsylvania, section at .... 108 
 
 Q- 
 
 Quakertown, Ohio, section near 191 
 
 Quakertown coal 201 
 
 Qainniinont coal 203 
 
 R. 
 
 Raleigh County, West Virginia, section in 142 
 Randolph County, West Virginia, section 
 
 in 151 
 
 Page. 
 
 Raymond City, West Virginia 56 
 
 Redstone coal 62 
 
 Redstone limestone 62-63 
 
 Red shale beds 92 
 
 Rice’s Landing, Pennsylvania, section at. 45 
 
 Richmond, Pennsylvania, section near... 115 
 
 “Ridge ” limestone, West Virginia 33 
 
 Ritchie County, West Virginia, section in 159 
 Roaring Creek coal vein, West Virginia. 151 
 Robinson’s Run, Monongalia County, 
 
 West Virginia, section at 46 
 
 Rock Point coal=Middle Kittanning coal 166 
 
 Rogers Brothers, strata named by 70 
 
 Rogers, H. D., strata named by 43, 59, 63, 147 
 
 section given by 103 
 
 Rogers’s subdivision of the Carboniferous 18-19 
 Rowlesburg, West Virginia, section near 188 
 
 S. 
 
 Sawpit branch of Cove Creek, West Vir- 
 ginia, section on 157 
 
 Scioto County, Ohio, sections in 134, 193 
 
 Scott’s Run, Monongalia County, West 
 
 Virginia, section at 47 
 
 Scrub-grass coal=Upper Clarion coal 175 
 
 Selby, A. G., section near Huntington, 
 
 West Virginia, furnished by 84 
 
 Serai conglomerate=Pottsville conglom- 
 erate 179 
 
 Sewickley sandstone 60 
 
 Sewickley coal 60-61 
 
 Sewickley limestone 61-62 
 
 Sewickley, Pennsylvania, sections at .... . 73, 112 
 
 Shade Creek, Ohio, sections at 66 
 
 Sharon coal 202 
 
 Sharon conglomerate 204-205 
 
 Shawnee limestone = Upper Freeport... 159 
 
 Shawnee, Ohio, section near 133 
 
 Shough’s Knob, Greene County, Pennsyl- 
 vania, highest Dunkard beds at.. 130 
 Shoup’s Run, Huntingdon County, Penn- 
 sylvania, section at 125 
 
 Sbumard, G. F., section furnished by 145 
 
 Simmons Creek, West Virginia 203 
 
 Simpson well, Wirt County, West Vir- 
 ginia, section 192 
 
 Sims, H. N., section given by 125 
 
 Somerset County, Pennsylvania, sections 
 
 in 121, 186 
 
 South Elk Horn Creek, West Virginia, 
 
 section on 203 
 
 Sprucevale, Ohio, section near 131 
 
 Steele, John L., section furnished by 189 
 
 Sterling mines near Houtzdale, Pennsyl- 
 vania, section at 124 
 
 Steubenville, Ohio, section at 77 
 
 Stevenson, John J., strata named by 31, 32, 33 
 
 34, 36, 37, 39, 59, 62, 88, 93 
 
 sections given by 44, 68,74, 116, 126, 149, 159 
 
 Stevenson, Wm. S., sections given by. . .78, 153, 185 
 Stone Coal Run, Upshur County, West 
 
 Virginia, section at 161 
 
 Stony Creek, Somerset County, Pennsyl- 
 vania, soction on 121 
 
212 
 
 INDEX. 
 
 Page. 
 
 Stoyestown, Pennsylvania, section at 121 
 
 Stroud Creek, West Virginia, section on. . 154 
 
 Sugar Camp Hollo-w, West Virginia, sec- 
 tion in 157 
 
 Summit limestone=Mahoninglimestone. 96, 97 
 
 Summit limestone=Upper Freeport 159 
 
 T. 
 
 Taylor County, ^ West Virginia, sectionsin. 128, 189 
 Taylorstown, Pennsylvania, section near. 30 
 
 Thomas, West Virginia, section near 127 
 
 Tioga County, Pennsylvania, sections in. 102,103 
 
 Tionesta coal= Upper Mercer coal 200-201 
 
 Tipton Bun coals, geologic place of 205 
 
 Trimble coal 167 
 
 Trough Creek, West Virginia, sections on. 157 
 
 Tucker County, West Virginia, sections 
 
 on 65, 82, 127, 187 
 
 Tug Fork of Big Sandy Biver, sections on . 146, 147 
 Twelve Pole Creek, West Virginia, sec- 
 tions on 156, 158 
 
 Tygart’s Valley Biver, section on 128 
 
 U. 
 
 Uniontown coal 59 
 
 Uniontown limestone 59 
 
 Uniontown sandstone 58-59 
 
 Upper Cannelton coal 97 
 
 Upper coal measures or Monongahela 
 
 Biver series 19, 42-69 
 
 table of beds of 57 
 
 Upper Freeport coal 147-148 
 
 Upper Freeport limestone 159 
 
 Upper Freeport sandstone 160 
 
 Upper Kittanning coal 164 
 
 Upshur County, West Virginia, sections 
 
 in 151, 152 
 
 V. 
 
 Valley Falls, West Virginia, section at . . . 128 
 
 W. 
 
 Wall, J. Sutton, section near Webster, 
 
 Pennsylvania, furnished by 68 
 
 Warfield coal, West Virginia 171 
 
 Warfield, Kentucky, section at 146 
 
 Washington “A” coal 35 
 
 Washington coal 37 
 
 Washington County, Ohio, sections in. . .29, 52, 192 
 
 Page 
 
 Washington, County, Pennsylvania, sec- 
 tions in 29, 45, 78, 113, 185 
 
 Washington limestone.. 35,36 
 
 Washington, Pennsylvania, sections at. 29, 77-78 
 
 113, 185 
 
 Washington sandstone..* 38-39 
 
 Wayne County, West Virginia, sections in. 155, 156 
 
 157, 158 
 
 Waynesburg “A” coal 39 
 
 Waynesburg “ B ” coal 39 
 
 Waynesburg coal 57 
 
 Waynesburg limestone 58 
 
 Waynesburg sandstone 40, 41 
 
 Webster County, West Virginia, section in 153 
 
 Webster, Pennsylvania, section near 68 
 
 Wellersburg, Pennsylvania, section near. 186 
 
 Westernport sandstone 59 
 
 W eller coal = Crinoidal coal 92 
 
 Wellsburg, West Virginia, section at 190 
 
 West Brownsville, Pennsylvania, section 
 
 at 45 
 
 Westernport, Maryland, sections near.. 56, 126, 186 
 Westmoreland County, Pennsylvania, sec- 
 tions in 44, 68, 113, 114, 116, 185 
 
 West Virginia Central Bailroad, sections 
 
 on 127 
 
 West Virginia and Pittsburgh Bailroad, 
 
 section on 152 
 
 Wetzel County, West Virginia, sections in 27, 38 
 Wheeling Creek, Pennsylvania, section on 24 
 
 Wheeling, West Virginia, sections at 130 
 
 Willard, E. B., record of boring furnished 
 
 by 193 
 
 Willey fork of Fishing Creek, Wetzel 
 
 County, West Virginia, sections on 38 
 
 Wilson’s mine, Bandolph County, West 
 
 Virginia, section at 151 
 
 Windy Gap coal 31 
 
 Windy Gap limestone 30-31 
 
 Winfield, West Virginia, section at 55 
 
 Winifrede, West Virginia, sections at 162 
 
 Wirt County, West Virginia, sections in 52, 83, 192 
 
 Wise, West Virginia, exposure at 34 
 
 Wood County, West Virginia, sections in. 130, 192 
 
 Wyoming County, West Virginia, sections 
 in 143,204 
 
 Z. 
 
 Zanesville, Ohio, section near 132 
 
 Zoar limestone = Upper Mercer limestone 200 
 
 o 
 
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5 GEOLOGICAL SURVEY 
 
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