I 
 
 A SKETCH 
 
 GEOLOGY, MINERALOGY, &c. 
 
 OF THB 
 
 CONNECTICUT 
 
 PART I. 
 
 The region embraced by the accompauying_inap, and to 
 which this sketch is principally confined, is about 150 
 miles long and 30 broad; extending from New-Haven to 
 'Bellows' Falls. A leading object of this map is to give an 
 /accurate view of the secondary tract extending from New- 
 Haven 110 miles northerly to Northfield. But it is protracted 
 30 or 40 miles beyond this, on the north, so as to embrace 
 probably all the argillite along this river. A considerable 
 extent of primitive is also exhibited on the borders of the 
 secondary. The map is not colored according to the Wer- 
 nerian distinctions of primitive, transition and secondary ; nor 
 according to Macculloch's division of rocks into unstratified 
 and stratified : but an attempt has been made to give every 
 particular rock that position and extent on the map which 
 it actually occupies on this portion of the earth's surface. 
 Every geologist knows, that perfect accuracy in these res- 
 pects, on a map of such extent, would require a degree of 
 labour and research, which, none but those whose whole 
 time is devoted to such pursuits, could bestow. Indeed, so 
 
 1
 
 2 Geology, &fc. of the Connecticut. 
 
 large a part of every country is covered with geest, and 
 so imperceptible is (he passage of some rocks into others, 
 leaving tlie observer in doubt for miles which rock predom- 
 ina'es, that after all, two equally good geologists would not 
 probably fix the limits of different rocks precisely alike. 
 And to exhibit all the minor salient and reentering angles 
 Avhich any rock makes on the surface, would require a map 
 on a scale five times larger than that used in the present 
 instance. In attempting, therefore, to give every rock 
 that position and extent on the map which it actually occu- 
 pies on the surface, I do not suppose I have done any thing 
 more than to approximate to the truth. It is hoped, howev- 
 er, that the approximation is sufiiciently close to answer 
 most of the purposes of geology. I trust at least that this 
 outline will furnish assistance to succeeding geologists. 
 
 In constructing this map I have derived very great assis- 
 tance in the vicinity of New-Haven, from the researches of 
 Professor Silliman, and of Dr. Percival. Indeed, could 
 either of these gentlemen have been induced to form a map 
 of that region, I should gladly have omitted the southern 
 part. In the northern part of the map, I have been assist- 
 ed by Dr. J. A. Allen, Lecturer on Chemistry in Middle- 
 bury College, and by Rev. J. Andrews, of Putney. Dr. 
 E. Emmons, of Chester, has also communicated facts of 
 importance. 
 
 The sides of the map are not precisely meridians ; but 
 incline 3 or 4 degrees to the right, as is evident from the 
 jleur de lis attached to the upper right hand corner. The 
 longitude and latitude are marked from those of Deerfield, 
 which have been determined by numerous observations. 
 
 Having made these preliminary remarks, I now proceed 
 to desoibe the several rocks occurring in this district, in the 
 order in which they are put down in the explanation of the 
 colours on the upper left hand corner of the map. 
 
 1. Granite. 
 
 Coloured jiurple — or a mixture of carmine, red, and 
 Prussian blue. 
 
 Almost every variety of this rock described by geolo- 
 gists occurs in the region of the map, except the transition
 
 Geology, SfC. of the Connecticut. 3 
 
 granite of Norway and Scotland. Its texture varies from 
 the coarsest to the finest grain, and it exists liere in most of 
 the forms that have been noticed. 
 
 East-Haven Granite, 
 
 The deposit of granite marked in East-Haven and Bran- 
 ford, has its southwestern extremity at the Lighthouse^ 
 which stands on a sea beaten rock of this description. The 
 grain is internfiediate between fine and coarse, and the fels- 
 par is usually reddish. In passing from East-Haven to 
 Branford, we find the granite immediately succeeding the 
 old red sand stone, or the slate rocks of the coal formation, 
 or the greenstone ; and all these rocks are nearly on the 
 same level. Their actual contact with the granite, howev- 
 er, has not been observed, being hid by geest. 
 
 There is no evidence tliat this granite constitutes a bed 
 in other rocks : On the contrary, it would seem, that it was 
 brought to view along the coast by tiie abrasion of the 
 gneiss and mica slate, which appear a few tniles to the 
 north, and which there lie at a much higher level. On 
 passing east and nortlieast from this granite deposit, well 
 marked beds of this rock appear; and perhaps all the gran- 
 ite which is found at the mouth of Connecticut river occurs 
 in this form. 
 
 I do not know exactly how far the East-Haven granite 
 may be traced along the coast. Certainly the gneiss reach- 
 es the sound before we come to Connecticut liver. 
 
 In the cavities of this granite, wheiicit is washed by the 
 tide, one or two species of hepas and other test {cea, have 
 fixed their abodes, finding security in those projecting crags 
 which are so appalling and dangerous to the mariner. Some 
 Ulvae and Fuci, also, are found along the shore. 
 
 South Hampton Granite. 
 
 Although the granite thus designated extends but a little 
 distance into South Hampton ; yet it contains the South 
 Hampton lead mine, which will, no doubt, be long an in- 
 creasingly interesting focus to which mineralogists will be 

 
 4 Geology, ^-c. of the Connecticut. 
 
 drawn — and (herefore, the specific name above given, may 
 not be unappropriatc for tliis granite. 
 
 A great part of this granite exists in beds in mica slate j 
 gneiss being a rare rock in the vicinity. Indeed, it may be 
 doubted whether the whole range is not in the form of beds. 
 I think, however, it will bo found that there is a central ridge 
 which is fundamental, at least two or three miles broad, ex- 
 tending from South Hampton through Williamsburg to the 
 southwest part of Conway and northeast part of Goshen. 
 Certainly, along this line little else appears but granite ; and 
 in some places, as at its northern extremity, this rock forms 
 hills of considerable elevation, and extensive ledgts. Beds 
 of granite may indeed be found in the vallies beiween 
 these ledges; but an observer as he passes o\'er this region 
 and proceeds south to South Hampton lead mine, will find 
 it difficult to persuade himself that he is not traversing an 
 original fundamental* deposit of this rock. Or if it exist 
 in beds alternating with mica slate, it will in some instances 
 be found no easy matter to prove it — the mere fact that 
 mica slate is found on both sides of it not being sufficient 
 evidence : the same being the case with an original deposit. 
 
 I would here suggest whether the mica slate of this re- 
 gion, that contains beds of granite, may not be a newer for- 
 mation, reposing immediately upon that granite nucleus 
 which probably forms the basis rock in New-England. 
 And wherever this mica slate and upper granite is worn 
 away, or there is a projection in the nucleus, the basis rock 
 may appear. Such a supposition will account for all the 
 appearances of the r^ion we are now considering, which is 
 coloured on the map as granite. 
 
 As we go east or west from what I have called the cen- 
 tral ridge of this granite, the beds of this rock become more 
 and more distinct, the mica slate, however, increasing in 
 
 * "The term fundamental, ha?, it should seem, been gratuitously predi- 
 cated of a particular description of granite ; for by the terms of the propo- 
 sition, the bottom of this formation has never been seen, and consequently 
 we have no means of determining whether it be fundamental or not." — Ed. 
 Rev. Jan. 1820, p. 89. 
 
 But, we should ask, whether it be not proper to say of space, that it is iu- 
 linite, for the very reason that we cannot limit it? And with equally good 
 reason, it would seem, we may say of granite that it is fundamental, be- 
 cause we have never found any other rock below a particular description 
 of it.
 
 Geology, ^c. of the Connecticut. 5 
 
 quantity and the granite decreasing. In painting what is 
 denominated the South Hampton granite, I have compre- 
 iiended most of the Chesterfield and Goshen granite,* which 
 has become celebrated on account of the interesting minerals 
 found in it — although the mica slate in those towns occupies 
 probably as much of the surface as the granite. The pur- 
 ple colour, or that which represents the granite, has not been 
 extended so far as to embrace all the beds of this rock in 
 Uiis region; but only so far as the granite predominates. 
 Where the mica slate is most abundant, I have put down 
 this rock as covering the whole surface, although it might 
 contain many beds of granite. 
 
 The inclination of the mica slate strata, or dip below the 
 horizon, and consequently of the granite beds, varies from 
 20° to 90°: and thus frequent opportunities are afforded for 
 observing the former rock pass under and over the latter. 
 The width of the beds varies from the fraction of an inch 
 to 100 rods: nay, perhaps to a mile or two. So that in 
 the narrow beds, a single glance of the eye will present their 
 roof and floor. In these thin beds there is rarely any fis- 
 sure; but in those several hundred yards in width, are fre- 
 quently observed regular and irregular divisions, as will be 
 more particularly noticed hereafter. 
 
 These distinctly characterized granite beds are not con- 
 fined to the region of the South Hampton granite. A (e\v 
 miles north, indeed, they disappear; but they may be 
 traced southerly into Litchfield county, where they exist 
 abundantly, and are sometimes found in hornblende, slate, 
 and gneiss. A good example of the former may be seen in 
 Granville, about half way between the churches in the east 
 and west parishes ; where the layers of hornblende slate are 
 nearly perpendicular. Instances of their existing in gneiss 
 may be seen in abundance on the east side of Connecticut 
 river, in Pelham, Monson, Chatham, Haddam, &tc. Indeed, 
 we think the geologist who traverses New-England primi- 
 tive rocks will often be led to enquire, whether all our gran- 
 
 * " We have visited these localities more than once, and have no hesitation 
 in sayins: that more distinct and well marked beds do not exist in this part 
 of the United States or Europe ; and what renders the fact more interes- 
 ting^ is, the distinctly stratitled structure of some of them." — J^'.Amer. Rev. 
 Ko. 29— p. 233.
 
 6 Geology, «yc. of the Connecticut. 
 
 ite does not (^ccur in the form of beds or veins. AVc arc 
 not yet, however, prepared to believe any one could con- 
 clude that it does. fc.ast-Haven granite. Black Mountain, 
 a part of Leverett range. &;c. stand as yet in the way of 
 such a supposition. Still less are v/e ready to adopt the re- 
 cent opinion of a distinguished European geologist,* that 
 granite is not a primitive rock, and that the only two rocks 
 that are so, are mica slate and gneiss! 
 
 Thus have we in New-England, as in the east of Ireland, 
 granite of a decided character alternating with mica slate. 
 But this ceases to excite any surprize, since Von Buch and 
 and Jameson have given us an account of the strata of Chris- 
 tiana and Haddington. t 
 
 The texture of the South Hampton granite is generally 
 rather coarse. There is, however, in this respect, a great 
 variety. The felspar is usually of a fine white colour, and 
 the quartz and mica a light gray. I do not here, however, 
 speak of the granitic veins, some of which traverse the 
 granite itself, and the felspar of which is sometimes flesh 
 coloured. The beds of the South Hampton granite are 
 not rich in minerals, except the lead mine in that town. 
 The veins in this rock, however, contain the fine tourmalines 
 and beryls of Chesterfield, and Goshen, and Haddam. 
 
 Black Mountain. 
 
 Thislies in Dummerston, Vermont, and consists of gran- 
 ite. A geologist standing in Braltleborough on the argillite 
 is surprized on looking northwesterly, and seeing only four 
 or five miles distant, an abrupt mountain 500 or 600 feet 
 
 * Dr. Borre. 
 
 t Porphyry in immeuse mountains reposing^ upon lime stone full of peti'i- 
 factioDs ; a sienite over this porphyry, consisting almost entirely of coarse 
 granular felspar, and in the same manner, a granite not different in its 
 composition from theo:ranite of the oldest mountains — granite «6ore transi- 
 tion limestone I Granite as a member of the transition Ibrmation I" — Von 
 Bucfis Travels in Noricay, p. 45. 
 
 Order of the transilion rocks around Christiana, beginning at the lop and 
 reckoning dowmcards. 
 I. Zircon sienite. 2. Granite. 3. Porphyry. 4. Sand stone. 5. Flinty slate. 
 6. Compact gray Waoke. 7. Compact slate and black orlhoceratite lime- 
 !tonc. 8. Granite. 9. Clay slate and limestone, probably. 10. Gneiss. — Ibd.
 
 Geology, <^-c. of the Connecticut. 1 
 
 high, evincine by its white and naked head that it is gneiss 
 or granite. On visit. ng it, he will find it to be a fino grained 
 granite. In many parts, howev -r, lie will perceive such a 
 tendency to stratification, that he may doubt for a mo- 
 ment whether it be not gneiss. But upon examination he will 
 refer it to sjranite. The same remark will apply to granite 
 in many other parts of New-England. It ?eems, and proba- 
 bly i?, in many instances, intermediate between well char- 
 acterized granite and gneiss. 
 
 Black Mountain is not many miles in circuit, and on the 
 north and west, is succeeded by well characterized gneiss. 
 This gneiss i-^ quarried and forms U'tderpinning and step 
 stones ; specimens of which may be seen in the foundation 
 of the Meeting house in Braitleborougb, East Village. 
 
 On Black Mountain 1 noticed some interesting lichens. 
 Th.e most monopolizit^g of these, are the Gysophoras. G. 
 vel/eo, papulose and mnklenhergii ; (Achariu.-) in some in- 
 stances actually cover precipices 30 or 40 feet high, and 
 crowd one another notwi hstanding, so as to force up their 
 broad margins, giving them the appearance of a chapeau de 
 bras. These species are found also on the granite in Mon- 
 tague, and on the greenstone in Deerfield, where occurs al- 
 so g. deusta. On Black Mountain I likewise noticed in 
 abundance Enclocarpon miniatum Ach. and several species 
 of Parmelin Qud Lee idea. Near its top grows Milium in- 
 volutum (nov. sp. Torrey, MSS.j 
 
 I cannot but detain the reader a moment to explain the 
 strange nomenclature by which those were governed who 
 originally gave to this granitic peak the name of Black 
 Mountain. Every body in passing is struck with its snow 
 jvhite aspect, and cannot help enquiring the cause of it. I 
 was told that in early days,<^ was burnt over and derived its 
 specific appellation from this circumstance. Thus an acci- 
 dental and ephemeral fact has fastened a name upon it 
 which its constant appearance belies. 
 
 A similar remark might be made in regard to the name 
 of another mountain in the same vicinity. A perion stand- 
 ing in Brattleborough East Village, perceives directly east 
 of him, on the east bank of Connecticut river, a venerable 
 mountain 800 or 900 feet high, seeming almost to threaten 
 him v/ith its overhanging fragments. On enquiring the
 
 8 Geology, fyc, of ilie Connecticut, 
 
 name of it, lie will be told it is West River Mountain. And 
 on examination lie will find that West River empties into 
 the Connecticut from (he west, nearly opposite this moun- 
 tain. 
 
 Granite range passing from Amherst through Levereit, ^c. 
 
 This granite is generally found at a low level. Almost 
 every other rock in the southern part, excepting the alluvi- 
 on, rises higher than this. Along the central and eastern 
 parts of Amherst it is mostly covered by geest and alluvion. 
 it appears, however, two miles south cast of the Collegiate 
 Institution, and I have no doubt that Seminary stands on 
 this rock ;*although some bowlders of pudding stone ap- 
 pear there. Two or three miles north of the College, it 
 emerges in abundance, and becomes broader through Leve- 
 rett, which is perhaps one of the best places for examining 
 it; especially when we consider its proximity there to pud- 
 diag stone. Mount Toby, which is 800 or 900 feet high, 
 lies on the western border of the granite and consists prin- 
 cipally of a peculiarly conglomerate rock which appears to 
 belong to the coal formation. This pudding stone rises 
 400 or 500 feet higher than the granite, and in the interve- 
 ning valley the two rocks approach very near each other ; 
 although I have never been able to find the actual junction. 
 The granite, however, near the pudding stone, occurs in 
 beds in mica slate, and is separated from the pudding stone, 
 by this mica slate, or by hornblende slate, which appears in 
 the valley above named, or by an imperfect variety of sie- 
 nite. The mica slate in this place, and indeed along the 
 whole western border of this range of granite, near the 
 northwest corner of the town, lit becomes mere qnartzose 
 slate, having a slight glazing of mica, or mica in small scat- 
 tered scales. This quartz is divided in two directions by 
 seams oblique to the face of the layers, so as to separate the 
 rock into very regular rhombs with different degrees of ob- 
 liquity. In hand specimens, indeed, it seems to be limpid 
 quartz in very perfect distinct concretions. 
 
 In the valley between these rocks appears to have been 
 for ages a war of avalanches between the pudding stone 
 and granite ; in which
 
 Geology, <^'C. of the Connecticut. 
 
 -'• hilh amid the air encountered hills, 
 
 Hurrd to and fro with jaculaliou dire," 
 
 And evidently too to the advantage of the pudding stone: 
 ibr this is several hundred feet the highest, is more steep and 
 more easily broken up from its bed, so that its debris has 
 evidently gained upon the older rocks, and subjected some 
 of them to its dominion. 
 
 In this valley the lichens, mosses and fungi, have planted 
 themselves thickly upon the bowlders and decayiiig logs 
 where they are secured by the dense foliage of the trees 
 fi-om the too powerful rays of the sun and moistened by 
 the vapour of a small brook which here finds a passage. 
 You there see Sticta pulmonacea (Ach.) and Jungermannia 
 platyphylia, fantastically fringing the rocks, v/hile the ever 
 verdant Polypodium vulgare frequently crowns the top. 
 Parmelia saxatilis, caperata, and others, several Lecanorcc 
 and Lecideae, Peltidea canina, Poiena pertusa Ramalina 
 fraxinea and Cenomyce cocdfera and rangiferinm of Achari- 
 us, Hedwigia fdiformis, Bartramia crispa, Polytrichum 
 perigoniale, several species of Hypnum, Dicianum, Ortho- 
 trichum, and many other genera grow there. On the de- 
 caying trees along this valley, you not unfrequently may 
 see the delicate Boletus versicolor and betulinus, the elegant 
 i?. cinnabarinus and htcidus, and the useful B. varius, velu- 
 tinus and igniarius, (Persoon.) Here too may be found 
 Agaricus alneus (Pers.) Dacedalea cinerea and Polyporus 
 abietinvs of Fries ; various Thelephorae, Hydra, Clavariac, 
 Pezizce, he. And the margin of the brook has in many 
 places a carpet of Marchantia polymorpha and conica. 
 Near the northern extremity of this valley is a pond, in and 
 around which are many rare and interesting phenogamous 
 plants — such as Drosera rotundifolia and longifolia, JVw- 
 phar advena and Kalmiana JSymphea odorata, Utricularia 
 striata (n. sp. Le Conte) Myriophyllum verticillatum, one 
 or two Charae, Cnicus lanceolatus, attissimus arvensis, dis- 
 color and muticus; Rhynchospora glomerata and alba J^u- 
 jas Canadensis and Scirpus ' subterminalis (n. sp. Torrey 
 MSS.) In the outlet to this pond grows the singular Spoil- 
 gia fluviatilis of Linnaeus. 
 
 But to return to the granite. Along the southern and 
 central parts of Montague, it is greatly hid by the gneiss and 
 mica slate. In the northern part of the town, however, 
 
 2
 
 10 Geology, ^c. of the Connecticut. 
 
 near the mouth of Milh^r's river, it appears in one or two 
 detached eminences of considerab'e heigl)t ; directly west 
 of wliich, only a few rods, is another hill of puddingstone 
 similar to that of Toby. The granite can be traced nearly 
 all the way through Northfield at a low level, and in 
 the north of this town it seems to pass under the geest and 
 higher rocks, and to appear again in Winchester and Ches- 
 terfield, of greater width, and here it is beautifully {)orph)^- 
 ritic. As we go north, the rock exists in distinct beds in mi- 
 ca slate and gneiss, and also it appears at the tops of moun- 
 tains sometimes forming conical hills almost naked. Wit- 
 ness the west j)art of Surrey and Alstead. 
 
 The texture of this granite is coarse, in some instances 
 very coarse, the plates of mica bei.'.g several inches across. 
 Its usual colour is white. A beautiful variety, however, 
 occurs in Leverett, in which the felspar, which is abundant, 
 is of a light blue; the quartz of a dark blue, approaching to 
 black ; and the mica the usual light gray. This a rare va- 
 riety, and a fragment of a crystal of this blue felspar meas- 
 ured in its longest direction 8 inches. 
 
 This range of granite contains several veins of metals, 
 such as galena, copper pyrites, blende and iron ; which will 
 be more particularly described hereafter. .^^ 
 
 Much of this range exists in the form of beds and'Mins: 
 yet so far as 1 have examined it, it will not be easy to prove 
 that the whole of it can be referred to this form. I am yet 
 of opinion that along the central parts of the range may be 
 seen emerging an original fundamental deposit of granite. 
 
 These are all the depositories of granite of considerable 
 extent, which I have discovered in the region embraced by 
 the map. Granite exists in many other places along this 
 river in beds and veins ; but not of sufficient extent to claim 
 to be represented on the map. It is possible, however, that 
 what I call beds and veins, may not in all cases be such : 
 For it is generally allowed, I believe, that the basis rock in 
 all New-England is granite, and this nucleus, if I may so 
 call it, is doubtless very uneven, having many prominences 
 and corresponding hollows. In some places, perhaps, these 
 projections have never been covered by other rocks, such 
 for instance, as black Mountain. In other cases there is 
 every appearance to indicate that the higher rocks have 
 been worn away, and thus the granite has been disclosed :
 
 Geology, Sfc. of the Connecticnt; 1 1 
 
 for in general, the granite along the Connecticut appears 
 much lowei" than the neighbouring rocks, such as s^neiss and 
 mica slate. No person who examines the East-Haven 
 granite, or that running through the Leverett, or even the 
 South Hampton deposit, will doubt that some powerful 
 agent has swept away an immense mass of superincumbent 
 rocks of some description or other. Whether this was a 
 piimeval northeasterly current as Mr. Hayden maintains, I 
 shall not undertake to decide. Be it, however, what it may 
 have been, wherever it has acted powerfully we may ex- 
 pect to find the granite laid bare. If these remarks are 
 correct, we need not be surprised to fisid this rock any 
 where, even if we cannot make it form any thing like con- 
 tinuous ranges, and perhaps some of those small masses of 
 granite, which every one who has examined New-Eng- 
 land knows, appear so frequently, and which being sur- 
 rounded by gneiss or mica slate, we are apt to refer to beds 
 or veins may, after all, be the top of a projection of tiie 
 nucleus of the globe which the abrading agent has laid 
 bare. 
 
 Belloivs Falls Granite. 
 r 
 This is of quite limited extent ; but the intcresling na- 
 ture of the spot where it occurs induced me to colour it and 
 notice it thus particularly. Fall mountain on the east bank 
 of the Connecticut at Bellows Falls, consists of a coarse, 
 not very perfectly stratified mica slate. At its western foot 
 in the bank of the river, ihc stratification becomes less dis- 
 tinct, and is at length, about the middle of the stream, en- 
 tirely lost; and the rock becomes an imperfect granite. In 
 other words, there is a graduation from the mica slate into 
 the granite. In the western bank, in the village, the char- 
 acters of the granite are more decided; though even here, 
 I should have no hesitation in calling it a sienitic granite, 
 did it contain any hornblende ; but I could discover none. 
 The mica is black and abundant, thus giving the rock a sie- 
 nitic aspect; and it is also traced by veins of felspar and 
 granite like the sienitic granite of Northampton and Belcher- 
 town, to be described hereafter. The ingredients of tnis 
 rock are arranged when viewed on a small scale somewhat 
 in distinct lavers : but when regarded as a whole. I never
 
 12 Geology, fyc. of the Connecticut. 
 
 saw a rock farther from stratification. Sometimes the fels- 
 par is wholly wanting, and the rock appears to be mere 
 unstratifed mica slate, if such a term does not contain a con- 
 tradiction. It is of no great extent, being evidently laid 
 bare by the waters of the Connecticut, which here urge their 
 way m foaming fury over its ragged cliffs. The same rock 
 occurs two miles east of the falls ; but, as far as I examin- 
 ed it, it seemed to occupy no great space. 
 
 Stratification of Granite. 
 
 rfzi 
 
 Probably the granite of .Connecticut will leave the ques- 
 tion* en this subject undecided. For some of it is evident- 
 ly stratified and some of it is not. That which exists in 
 not very extensive beds exhibits, so far as I have examined 
 the subject, the most decided marks of stratification. It is 
 not unfrequentto see the bed divided into layers parallel to 
 its roof and floor, and from one foot to two feet thick. This 
 is readily distinguished from gneiss by the much greater 
 thickness of the layers and the want of a stratified arrange- 
 ment of the ingredients. In other instances, more rare, 
 however, we observe what Saussune would call vertical 
 plates (feiiilhts) — that is, thick tables of granite perpendi- 
 cular to the horizon, crossing the bed sometimes at right an- 
 gles and sometimes obliquely. These plates are also found 
 making a dip to the horizon — In all these cases, however, 
 the plates being parallel, or nearly so, the rock would be 
 properly denominated stratified. Examples of these vari- 
 ous kinds of arrangement may be seen in Conway, Wil- 
 liamsburg, Goshen, and Chesterfield. Yet the greater part 
 of our granite is divided by numerous fissures into these ir- 
 regular blocks that bid defiance to precise description. 
 
 Granitic T^eins. 
 
 By veins I understand those zones of any particular 
 rocks, or mineral, which traverse another rock, either rec- 
 tangularly or obliquely to the direction of its strata. In 
 crossing the strata they differ from beds. 
 
 * See Greenough's First Principles of Geology. — Essay 1.
 
 Geology, Sfc. of the Connecticut. 13 
 
 Granitic veins are very numerous in many parts of the 
 map, especially in the region of the South Hampton granite. 
 In width they vary from a mere Hne to 30, and perhaps 
 even 40 feet. But I have not observed any that exceed 
 this breadth. They traverse mica slate, hornblende slate, 
 limestone of a peculiar character, sienite, gneiss and gran- 
 ite. Those which traverse the latter rock differ from it only 
 in being of a finer, or a coarser grain. Yet they are as re- 
 ally veins as those zones of granite traversing other rocks. 
 Examples of these are frequent — as near the South Hamp- 
 ton lead mine. , 
 
 In these veins all the ingredien.ts of granite are usually 
 present, but in variable proportion. I have seen some that 
 were nearly or quite graphic granite : But usually the mica 
 is in superabundance, especially in the narrower ones, and 
 often it is of a delicate straw or light green colour, as in Go- 
 shen and Conway. The felspar is sometimes of an ele- 
 gant flesh colour, especially in those veins occurring in the 
 gneiss northeast of New-Haven, in Chatham, Haddam, ^c. 
 These veins frequently divide and subdivide like the top of 
 a tree, some of the branches being smaller and some larger. 
 These branches rarely go ofF from the main stock at right 
 angles, but generally oblique. At one place you will see a 
 vein retaining its width for several feet, or even rods, with 
 mathematical exactness — at another, its width will gradually 
 increase or decrease; and I have seen, in some instances, a 
 sudden reduction of two or three inches, by which a shoul- 
 der was produced. The course of many of these veins is 
 serpentine, resembling that of a river on a map — yet often 
 they scarcely deviate at all from the right line. Some- 
 times they make large curves to the right or left. They 
 usually descend into the rock obliquely to the horizon. 
 They frequently intersect, but I have never noticed any dis- 
 placement of the strata, or mass of the rock, except in the 
 sienite. Some of the veins traversing sienite, (between 
 Belchertown and Ludlow for example,) are so numerous 
 and their intersections so many, that they form what the 
 Germans call a stock ivorke, except that they are not metal ■ 
 ic. By these cross veins the surface of the rock is some- 
 times divided into triangles, rhombs, or rhomboids; and 
 sometimes it is tesselated.
 
 14 Geology^ &fc. of the Connecticut. 
 
 The veins traversing seinite are most frequently granite, 
 -fAi- felspar being of a flesh colour. They are more numerous 
 in this than in any other rock, and are often intersected by 
 one another and by thin veins of epidote. The crossing of 
 these veins has produced many very interesting and singu- 
 lar displacements of portions of the rock. Where one 
 vein is cut off by the intersection of one that is newer, it 
 is not unfrequent to observe a lateral removal of the former 
 with the whole mass of the rock surrounding it, from one 
 to six inches. The vein itself, which is thus removed, is 
 rarely altered or injured. 
 
 One of the most complete and curious cases of this kind 
 is exhibited in Fig. 6. It was sketched by the eye without 
 accurate admeasurement. A. B. C. is a triangular mass of 
 sienite; the sides of- which are 6, 4, and 10 feet. A.B. is a 
 fissure in the rock : B. C. a vein of epidote and A C. the 
 line marking the lowest limit of the rock above the soil. 
 The whole rock is unbroken and as firmly united as any 
 rock of this character ever is. There appear originally 
 to have been two veins of granite traversing the rock in its 
 longest direction, the smallest an inch wide at one end and 
 widening towards the 'ither, and the longest 2 or 2 1-2 wide. 
 These have been cut through and strangely displaced by nn- 
 merous veins of epidote crossing obliquely. 
 
 a, «, a, and b, h, b, &ic. represent the granite veins as 
 displaced. 
 
 d, d, d, he. represent the veins of epidote which are 
 rarely more than one quarter of an inch thick, and a few of 
 which are represented on the plate. 
 
 c is a mass of gneiss or mica slate imbedded in the sienite 
 and crossed by the granite vein b. 
 
 The locality of this rock will be described when we come 
 to speak of sienite. 
 
 In those rocks that are stratified these veins make every 
 possible angle with the direction of the strata. And if I do 
 not mistake, the nearer they approach to the same direction 
 as the strata, the broader they become, and liave a nearer 
 resemblance to beds. Sometimes they approach so near 
 the same course as the layers of the rock they traverse, 
 that it requires nice examination to determine whether they 
 deviate at all. A good example of this occurs in a locality 
 which many geologists have visited, and which many more
 
 Geology, ^c. of the Connecticut. 15 
 
 will probq^ly visit. I refer to the main body of that enor- 
 mous vein containing the green tourmalin, rubelite, &ic. 
 in Chesterfield. We thinly it might even admit of a ques- 
 tion whether this be a bed or a vein. 
 
 The veins of which we are now speaking are doubtless 
 contemporaneous ones — that is, such as were consolid Jted 
 at the same time with the rocks they traverse. There is no 
 seam or layer of another rock at their sides, but they are 
 usually so firmly united to the rock which contains them, 
 that they are separated from these with as much difficulty 
 as they are broken in any otner direction. I have, how- 
 ever, frequently noticed a seam traversing the middle of the 
 vein — so that if the rock they traverse be broken up, one 
 half will cleave to one side and one half to the other. 
 
 A real lusus naturae exhibiting the fijBB^cohesion of these 
 vems to the rocks they traverse, now lies before me. A slab 
 of granite being a vein 2^- inches thick, lO inches broad, and 
 20 inches long, curved a little upwards at one end, forms 
 the base of the specimen. From the centre of this, rises 
 perpendicularly a bladed, taper-pointed column of a pecu- 
 liar limestone, only 2 inches thick, 10 inches broad at the 
 base, and 26 inches high, appearing as if mortised into the 
 granite. The contrast between the light coloured granite 
 and the dark gray limestone, is very striking. The secret 
 of its having been brought into this singular form appears 
 to be this. It was found in a mountain torrent in Conway, 
 and the granite doubtless once formed a vein in the lime- 
 stone. On one side the limestone has been entirely worn 
 away by the water — and on the other side, it is worn so as 
 to leave only the bladed column above described, which 
 still adheres firmly to the granite. 
 
 T have said that these granitic veins are contemporane- 
 ous ones : And it would seem that the judgment of no man 
 could be so warped by theory, as to believe, after examin- 
 ing them, that they were once fissures made in the rock? 
 they traverse, after these were consolidated, and that these 
 fissures were filled by a solution of water above, or by a 
 fiery furnace beneath. There is just as much reason for 
 believing that one of the constituents of granite, quartz for 
 instance, was introduced into the rock in this manner after 
 the other constituents were consolidated; or that the imbed-
 
 1 6 Geology, ^c. of the Connecticut. 
 
 ded crystals of porphyry are not of the same ag^with the 
 base. 
 
 Granitic veins are numerous in many parts of the map. 
 Commence at Conway and go south, and they will be 
 found in abundance nearly to the ocean. North of this 
 town I have never noticed any. On the east side of Con- 
 necticut river, also, they are not unfrequent, particularly in 
 Connecticut. Many of the interesting minerals of Had- 
 dam and Chesterfield occur in them. 
 
 Veins of quartz are sometimes seen in this region tra- 
 versing granite, as in Conway. But they are not extensive, 
 or numerous. I have noticed also that sometimes the gran- 
 ite contains, imbedded in it, masses of mica slate having a 
 curved form and not rounded ; as on the top of the high 
 bill between Williamsburg and Chesterfield. ^ 
 
 Graphic Granite. 
 
 This is a rock not uncommon in the region of the map. 
 I shall notice two of the finest localities. The first is in 
 the red conglomerate, or coarse sand stone, passing through 
 Deerfield. The imbedded masses in this rock are some- 
 times the most beautiful graphic granite. The felspar, al- 
 though it retains its lustre most perfectly, appears to be 
 thoroughly penetrated by the colouring matter of the con- 
 glomerate so as to become of a deep flesh colour. The quartz 
 is gray and limpid, or a little smoky, and being arranged 
 s^omewhat graphically, many of the specimen are truly ele- 
 
 The other locality of this rock, is the Goshen granite, 
 in the northeast corner of the town. The felspar is of a 
 snow white, and the quartz limpid; and so perfectly graphic 
 is its arrangement, that it bears a close resemblance to the 
 Chinese or Hindostanee characters which are frequently 
 observed on goods from the East-Indies. 
 
 Porphyritic Granite. 
 
 This handsome rock occurs in great abundance in loose 
 rolled pieces along the range of granite passing through 
 Leverett, &c. The crystals of felspar are from one to two 
 inches long, and a half or three quarters broad, and some-
 
 Geology, 8^c. of the Connecticut. 17 
 
 times the fpw; presented is a square. Thus an idea is con- 
 veyed to the observer, at first, that the crystals are rectan- 
 gular parallelepipeds and cubes; although it is well known 
 that felspar never crystallizes in either of these forms. 
 The felspar of these imbedded crystals, when broken, ex- 
 hibits the pearly lustre of the folia very well The granite 
 containing these cr) stals is almost uniformly of a coarse tex- 
 ture. 
 
 This porphyritic granite is carefully to be distinguished 
 from glandulous gneiss, which also occurs abundantly along 
 the Connecticut. Let any one pass from Hinsdale, New- 
 Hampshire to Winchester and he will see numerous bowlders, 
 often ten feet diameter, of a rock having the granite constit- 
 uents and exhibiting no appearance of a schistose structure. 
 In one place at least he will cross the rock in place ; and he 
 will have no doubt that it is the most decided granite. And 
 yet it is elegantly porphyritic. This rock occurs also in 
 Chester where Dr. Enmiovs has traced a range of it five or 
 six miles. Numerous bowlders of this rock are scattered 
 over the town of Woodbridge near New-Haven : but I do 
 not know from whence they originated. 
 
 Pseudomorphous Granite. 
 
 I put this adjective to a variety of granite that occurs along 
 the Connecticut, not to show my dexterity at coining new 
 terms, put to make myself understood. I am inclined, how- 
 ever, to think that the rock to which I refer is not exactly de- 
 scribed in the geological books which I have seen, unless 
 it be by Cleaveland, when he says, " som^ varieties (of gran- 
 ite) are divisible into imperfectly columnar or tabular con- 
 cretions." (Mineralogy, vol. 2, p. 7^12.) It is a coarse 
 grained granite with light coloured quartz and feldspar, ar- 
 ranged in the usual manner. The peculiarity lies in the mi- 
 ca. This is usually dark coloured, and arranged in plates 
 from one to three inches across. The manner in which 
 these are disposed, may be thus explained. Suppose the 
 quartz and felspar to have been cemented togpther so as 
 to form a perfect graphic granite. Next suppose the mass 
 to be cut in various directions by a fine saw j and in the 
 spaces thus made, imagine thin plates of mica, not more 
 ihan /, of an inch thick, to be fitted. Tt is obvious thatthe 
 3
 
 18 Geology, &,'c. of the Connecticut. 
 
 mass will thus be cut up into segments of pseudomorphoua 
 crystals. And so it is in the natural specimens: and it 
 seems as though the hand of nature had really made use of 
 a saw in their construction. The plates of mica meet at 
 various angles, yet never cross each other; and the smallest 
 piece of quartz or felspar is sometimes bisected, so that a 
 part appears on one side of the plate of mica and a part on 
 the other. This rock occurs in the S. Hampton granite ; 
 and may frequently be found in other parts of the region 
 extending fifty miles south from Conway. At a little dis- 
 tance the dark bronze coloured mica appears like prisms of 
 some imbedded mineral : and the travelling geologist is of- 
 ten tempted from his carriage in the almost certain expecta- 
 tion of obtaining from this rock shorl or titanium. 
 
 2. Gneiss. 
 
 Colourcil Orange. 
 
 Although this is the most abundant rock in New-England, 
 yet the map includes no very extensive portion of it. It 
 stretches over a broad region without the limits of the map 
 on the east and west, especially on the east. On the west it 
 forms a part of the Hoosack or Green Mountains; though a 
 much less part than has been usually supposed. On the east 
 i^appears with some interruptions of granite, mica slate, &:c. 
 within twenty or thirty miles of the coast, and on the north 
 it spreads over a considerable part of New-Hampshire. 
 The White hills are said to consist chiefly of this rock : 
 though they have not, 1 believe, been thoroughly explored. 
 
 The dip of the layers of gneiss in this re-;ion varies from 
 20° to 90° — and it dips, like most other stratified rocks along 
 the Connecticut, to the east. When it approaches to horn- 
 blende slate the dip is generally greater than when pure. 
 This rock often contains crystals of hornblende ; in every 
 proportion, indeed, until the characters of gneiss are lost in 
 hornblende slate. Especially is this the case on the cast 
 side of Connecticut river. More, however, will be said on 
 this subject when we come to describe hornblende slate. 
 Good examples of this gneiss containing detached crystals and 
 even veins of black hornblende may be seen in the base- 
 ment of the new Collegiate Institution in Amherst. It fur-
 
 Geology, ^c. of the Connecticut. 19 
 
 wishes an admirable stone for such purposes ; and many- 
 quarries are opened in it. Immense tables of it may be 
 procured, and should the mania for constructing pyramids 
 ever seize the inhabitants of New-England, this gneiss might 
 produce masses of stone rivahng in magnitude the im- 
 mense limestone blocks of the pyramids of Egypt. 
 
 The gneiss of the Connecticut, often alternates with mica 
 slate, and passes into it. In Granville, may be seen gneiss, 
 hornblende slate and mica slate, in various stages of ap- 
 proach to each other, and making various alternations. 
 
 This mixture of gneiss with other rocks, and the consequent 
 indistinctness of character, render it, in some instances, not 
 very easy to give its limits. I have felt this dj^culty espe- 
 cially in regard to the northern part of that gneiss range 
 which occupies the eastern part of Litchfield County and 
 appears so decided in its characters in Bristol, Plymouth, 
 and Canton. In the west part of Granville, I feel confident 
 gneiss is the prevailing rock — although mica slate alternates 
 with it. Yet between Chester and Wesifield there is nothing 
 but mica slate, as the prevailing rock, which extends twelve 
 or fourteen miles west of Chester, before we come to gneiss. 
 And north of this we find very little gneiss within the limits 
 of the map except a narrow stratum as we ascend the hill 
 from Cummington to Goshen. I do not, therefore, feel ex- 
 actly satisfied with the northern termination of the Litch- 
 field gneiss as given on the map : but at present it is not in 
 my power to re-examine it. 
 
 1 would here, however, suggest that I have been rather 
 inclined to believe that some of the stratified rocks along 
 the Connecticut pass gradually into other rocks laterally, 
 that is, in the direction of the strata: — mica slate, for in- 
 stance, into gneiss, or hornblende slate; and argillite into mi- 
 ca slate. To establish this fact, however, requires a long 
 series of very close and accurate observation. I merely 
 suggest it, therefore, and do not assert it. 
 
 In some instances, the ingredients of our gneiss are pret- 
 ty equally mixed: in others they are arranged in somewhat 
 distinct layers, which are generally straight. It is not a 
 rock that is rich in minerals with us. Veins of granite tra- 
 versing it, however, sometimes contain interesting specimens. 
 Witness the Haddam minerals.
 
 Geology, ^c. of the Conneclicvt. 
 
 Glandulous Gneiss. 
 
 This is very abundant, especially in the gneiss east of 
 Connecticut river. Indeed, a considerable proportion of 
 that range is occasionally glandulous, presenting numerous 
 oval masses, chiefly of felspar. The layers of this variety 
 of gneiss are usually very distinct, and it contains a large 
 proportion of mica, which is usually of a blackish colour; 
 and thus it is easily distinguished from the porphyritic gran- 
 ite above described. 
 
 3. Hornblende Slate, Cleaveland. 
 
 Coloured Vermillion, Red, and clouded with India Ink. 
 
 This is an anomalous and perplexing rock. It is not 
 generally well characterised in this region: but I have put 
 it down, because a rock approaching nearer the characters 
 of this than of any other, occurs in considerable abundance 
 along the Connecticut. I have no confidence however that 
 I have given in all cases its exact situation or extent. Yet 
 I believe that wherever this stratum is coloured on the map, 
 the rocks may be found in the vicinity. Thus in the range 
 extending from Belchertown to Guilford, Ct. a person willgen- 
 erally find this rock more or less abundant in crossing from the 
 secondary rocks to the gneiss : but sometimes he may thus 
 cross and miss of it, unless he make an excursion to the right 
 or left; and sometimes he must cross a portion of the gneiss 
 before he reaches it. The continuity of the strata of this 
 rock seems to be much less perfect than in the gneiss or 
 mica slate, and the direction of the strata if often oblique to 
 that of other rocks : — a remarkable instance of which occurs 
 in the south east corner of Halifax, Vt. The dip of the 
 strata varies from 45° to 90', and the schistose structure in 
 the purest specimens is very perfect, the layers varying in 
 thickness from half an inch to three inches. 
 
 But there is another difficulty in ascertaining the limits of 
 this rock. It is no easy matter to draw the line between it 
 and gneiss, all, or at least, two of the ingredients of the lat- 
 ter rocks bein^ sometimes present, while more than half of 
 the rock is hornblende. Indeed, I have sometimes been dis-
 
 Geology^ SfC. of the Connecticut. 21 
 
 posed to regard this rock as gneiss containing an accidental 
 proportion of hornblende ; and this would have been a satis- 
 factory description of a considerable part of the rock which 
 I have called hornblende slate. But another part appears 
 to be decidedly that species of V\ erner's primitive trap de- 
 scribed under the name of hornblende slate in Rees Cyclo- 
 pedia, Article Trap — that is, it consists of hornblende, gen- 
 erally fibrous and crystalline, having a very distinctly slaty 
 structure. For localities of this well characterized horn- 
 blende slate I would mention the eastern part of Halifax. 
 Vermont, also New Fane and Belchertown, two miles north 
 of the meeting house on the west side of the road, and in 
 the western part of Tolland and Monson. 
 
 I think however that the largest part of this rock will be 
 found to consist of hornblende, quartz and mica — the latter 
 being usually black and very apt to be confounded with the 
 hornblende, so that perhaps it deserves the name of a granitic 
 aggregate. In some instances, also, this rock contains chlo- 
 rite, and verges towards greenstone slate. It is often 
 strangely intermixed, and alternates with gneiss and mica 
 slate. 
 
 Another portion of this rock has a porphyritic aspect. 
 I use the term porphyritic in this place, not in the usual 
 sense, as denoting a compact ground with imbedded crys- 
 tals, but as a "granite ground, in which some crystals are 
 much larger than the rest." {BukeweWs Geology, p. 28.) 
 The slaty structure of the rock, though less distinct, is not 
 lost : but the imbedded fragments, or imperfect crystals of 
 quartz or felspar, most frequently the former, give it a 
 porphyritic appearance. These imbedded fragments arc 
 frequently granular, while the base is distinctly crystalli- 
 zed. A good ejEample of this variety of rocks occurs in the 
 west part of Chatham and in Shelburne. Sometimes this 
 rock becomes the real sienitic porphyry of authors — its 
 slaty structure being lost. This occurs in Plainfield, in 
 Hawley, a few rods west of the meeting-house, and at the 
 falls in Deerfield river in Shelburne. 
 
 These porphyritic rocks, however, must be quite different 
 from any thing occurring in Europe by this name, if a re- 
 mark of Brongniart be correct, that " we are not at present 
 able to find a sienite or porphyry which is evidently primi- 
 tive." For we have as much evidence of the primitive char-
 
 22 Geology^ fyc. of the Connecticut. 
 
 acter of the rocks above described, as of the mica slate and 
 gneiss with which they are associated and in which they 
 sometimes form beds. 
 
 Hornblende slate occurs on the west side of Connecticut 
 river, south of Shelburne, in Massachusetts and Connecticut, 
 also at Plainfield and Hawley. But it is not abundant or 
 well characterized generally, and is much mixed with, and 
 passes into other rocks; and therefore I have coloured it 
 only in the range from Belchertown to Guilford and from 
 Shelburne northward. Good examples of the rock contain- 
 ing quartz and some mica may be seen in tb^ flagging stone 
 of the side walks along the eastern side of the PubUc Square 
 in New-Haven, and in other parts of that city. 
 
 4. Mica Slate. 
 
 Coloured Green. 
 
 This is an extensive stratum in the northern part of the 
 map. On the west side of the river it forms the prevailing 
 rock; and its width continues to increase northerly, so that 
 it occupies the principal part of Vermont. Prof. Silliman in 
 his " Tour between Hartford and Quebec," says that he 
 crossed this st&te obliquely from Burlington to Hanover, a 
 distance of 84 miles, and found mica slate by far the most 
 abundant xock on the route. {Tour, &.c. p. 386.) In Con- 
 necticut, however, along the river, this rock constitutes no ve- 
 ry broad ranges. Those which are coloured immediately in 
 contact with the secondary on both sides of the Connecticut 
 are in most places quite narrow, often not more than half a 
 mile, or even but a few rods wide, and sometimes they whol- 
 ly disappear and we pass from the sandstone immediately to 
 the hornblende slate or gneiss. 
 
 The dip of our mica slate is variable from 20° to 90"^. In 
 Vermont it is usually less than in Massachusetts; especially 
 where we first strike it in passing from the river. Farther 
 south, as in Hn^ley, Plainfield, Chesterfield, &;c. it approach- 
 es 90°. East of Chesterfield the layers of this rock lean to 
 the west. Beyond Chesterfield, on the west, they lean the 
 contrary way — that is, to the east. The same is the case 
 between Chester and We^tfield. This fact looks like an 
 indication of a fundamental ridge of granite, extending in
 
 Geology S^-c. of the Connecticut. 23 
 
 that direction, as we have already suggested; ahhough it 
 may not yet have made its appearance above the later rocks 
 the whole distance. 
 
 This rock is somewhat Protean in its appearance; yet 
 not very difficult in most cases to be distinguished by care- 
 ful observation. The following varieties have been noticed 
 in this region. 1. A variety already referred to, as occur- 
 ring in Leverett, near the pudding-stone; which is scarcely 
 any thing more than imperfectly limpid quartz, divided into 
 distinct rhombic concretions, about an inch thick, and three 
 or four across the outside, slightly spangled or glazed with 
 mica. 2. Very much like the last, except that it does not 
 divide into complete rhombs, but is only separated by seams 
 oblique to the direction of the strata, and nearly perpendic- 
 ular to the horizon* — Locality, West-River mountain in 
 Chesterfield New-Hampshire. 3. Divided as the last by 
 two sets of parallel planes, forming angles with each other a 
 little oblique: But the mica is intimately disseminated in 
 fine scales through every part of the rock, and the quartz 
 becomes a mere siliceous sand, blended closely with the 
 mica." Surface rarely waving — Locality, Whately, Con- 
 way, he. 4. Not regularly divided in any direction, ex- 
 cept that of the strata, and much less fissile than the last. 
 Mica scattered in fine scales through the mass, and the silex 
 more abundant than the last — Rock breaking into huge 
 blocks, from one to three feet thick, and often forming, like 
 greenstone, abundance of debris. Locality, West-River 
 mountain and Deerfield. These four varieties occur on the 
 borders of the secondary rocks. 5. Tortuous, wavy and 
 extremely irregular, embracing numerous beds and amor- 
 phous masses of quartz — Mica, very imperfectly character- 
 ised, forming a kind of glazing with the aspsct of plumbago. 
 Locality, Conway, Shelburne, Colrain, he. 6. Quartz and 
 mica in somewhat distinct layers — quartz predominating, 
 and mica not very well characterised — abounding in garnets 
 — Locality, Plainfield, Hawley, Conway, &:c. 7^ Passing in- 
 to talcose slate — mica abundant, having somewhat of a fi- 
 brous aspect and connected with talc. Northfield and Haw- 
 ley. 8. Passing into argillite. Locality, Leyden, Ches- 
 
 *"When one set of parallel planes crosses another, are both sets to be cal- 
 led strata, or neither, or only one. of them ?" — Grefnmiglis Geology, Essnij 1 ,
 
 24 Geology, ^c. of the Connecticut. 
 
 terfield, (N. H.) Putney, &ic. 9. Not very fissile — break- 
 ing into thick blocks. Mica, abundant but poorly charac- 
 terised — having somewhat the aspect of argillite — surface 
 slightly irregular, appears as if grooved — Abundant in Cura- 
 mington, Chesterfield, (Mass.) Vernon, Bolton, &,c. 10. 
 Quartz granular, abundant and white — resembling gneiss 
 or granite — scarcely stratified at all — Locality, Buckland, 
 Granville, &;c. 11- Mica in distinct and abundant plates — 
 layers very little tortuous or uneven. This usually lies next 
 to granite. 12. Passing into gneiss — often rendered por- 
 phyritic by crystals of feldspar. Locality, Litchfield county. 
 
 The quartz that occurs in this mica slate, especially in 
 the wavy and tortuous varieties, is commonly the white 
 limpid: frequently it is the fetid, and sometimes a rich vari- 
 ety of a delicate red color. The coloring matter, however, 
 is apparently iron, and therefore it is not the rose-red quartz. 
 This variety of quartz occurs on the west side of the Con- 
 necticut. 
 
 It has already been remarked, under granite, that nu- 
 merous beds of this rock are contained in mica slate. In- 
 deed, our mica slate more frequently rests immediately up- 
 on granite, without the intervention of any other rock, than 
 does gneiss. It also alternates with gneiss, hornblende ^ 
 slate, argillite and chlorite slate. Small paQa^B of it, m-7oh^ 
 deed, occur in very many places throughout the whole ex- 
 tent of the primitive along the Connecticut. 
 
 It is a common remark in geological books, that hills | 
 
 composed of mica slate are usually less steep and more 
 rounded than those of granite. But the reverse is the fact 
 in most cases along this river. The granite hills are gener- 
 ally low and rounded, while some of the most Tarpeian 
 precipices to be found in this region are composed of mica 
 slate. Take for examples West River Mountain, and the 
 high hills of Heath, Hawley, Chesterfield, &;c. \ 
 
 Mica slate is not wanting in a variety of minerals in this ^ 
 
 section of the country— -such, for instance, as staurotide and 
 garnets in immense quantities in Goshen, Chestorfield, 
 Mass. and from Bolton, Conn, one huudred miles north, to 
 Chesterfield, New-Hampshire Also the fine Chesterfield 
 sappare. Also the red oxid of titanium, found almost -jv- 
 ery where between Conway and Brattleborough, a distance 
 of thirty miles — and the Leyden tremolhe — the Putnev
 
 Geology i 4"C. of the Connecliciil. 25 
 
 ^reen fluor spai-, and the Wardsborough zojsite. The 
 Chatham Cobalt mine occurs in mica slate. 
 
 The cryptogamoiis plants that usually o\ erspread a great 
 part of the mica slate of this region, though perplexing to 
 tJie mere geologist, are yet interestij^ to the botanist. 
 Among those which adhere to these rocks, or to the litdc 
 soil that collects in their cavities, may be named, Barira- 
 mia gracilis, Smith, B. longistta, J\Jx? B. crispa, Swnrtz, 
 Ilechoigia Jiliformis, P. Beuv.v. in great abundance; Arrlie- 
 nopterum heterosttcum, Hedw. Buxbaumn aphijUa, Lin. 
 Fissidem adianthoides, Bryum roseum, Diphyscium folio- 
 sum, Spreng. Pcli^trichian perigoniale, JMx. Jungermannia 
 comptanata, L. J. platyphylla L. Cenomyce phyllnphora, 
 and pyxidaia, Ach. Stereocanlon pasch cle, Parmd a herha- 
 cea,saxatilisandc:!peraia,Porinopnpillosa,andper!i(sa,Ptlti' 
 dea aphlhosa and scutata, and Sticta pulmonacea, all of 
 Achari(!S. In the region of the mica slate, especially in 
 Brattleborough and Conway, we frequently find Bryvm 
 cuspidatu7n,Brid. Hypnum minutuium,J\Ix. H. flexile, Brid. 
 11. serpens, L.H. cupressiforme,H'^hi'. Jungermannia nodifo- 
 lia,Torrey,Maschalocarpus trichonitrion, Hed. Pterigoniiim 
 subcapillatiim,Brid. \eckcra minor, Brid. TV'. pennata,Hed. 
 J\\ viticulosa,Hed. Cenomyce coccfra, rangiferina, hotrys, 
 ^c. — Parmelia^^ colpodes, nlnthrix, cyc/ocelis, parietina, 
 plumbea, S^'C.^^Lecanora tubercidata, subfnsca, brunnea. al- 
 bella, &fc. — Lecidea parascena, cameoln, demissa, ^^c. — Us- 
 nea florida and plicata, Cornicularia fibrillosa, Collema iu- 
 naeformis, and Alecioria jubala, all of Ach. Kephroma resu-- 
 pinata, Sprcvg.G Ionium stellnre,A]uhl. Pohjporus ubietinus 
 and sqvamosus. Fries. Hydnum giiercimim and cyathiforrae, 
 Fries. H. imbricatum, occanum, coralloides and gelatinosum, 
 Pers. Thelephora quercina and terrestris, Cyathus alia and 
 striata, Stemoniiis ftsciculata, Boletus citrinns, badius, bru- 
 malis, nigro-marginaius, cinncbnnnus, velutinus, betulinns. 
 ^c. all of Persoon, and many scores besides o^ Airaricus, 
 Amanita, Sphaeria, Peziza, Daedalea, Helvella, Lycoper- 
 don, Bovista, Scleroderma, Trcmella, ^'c. too numerous 
 to mention in thi^ place. 
 
 Scattered among the mica slate rocks we frequently find 
 
 the Hdix alloL\b,'is, Say, or common snail; and also, in 
 
 some situations, II. idternata, Sny. In a pon-;-. in Ashfield 
 
 is found Planorbis bicarincitus, Say,^nd Cyclassimih's,Say. 
 
 4 
 
 \
 
 26 Geology, (^c. of the Connecticut, 
 
 In springs occurs a species of Lymnaca, Scry, and in our lar- 
 ger streams, Planorbis trivolvis and Vnio purpureus, Say, 
 or common river clam. 
 
 V 
 
 5. Talcos» Slate. Rees Cyc. Bukewell, 
 
 Talcose Schist. Alaccullock. 
 
 Talcose Slate. Eaton. 
 
 Colored Gamboge yellow, and dotted icith India Ink. 
 
 Bakevvell defines this rock to be "slate containing talc," 
 (Geology, p. 491,) and Eaton calls it "that kind of mica slate 
 which is distinguished from mica slate by a kind of talc 
 glazing.'' In this term I do not include soapstone. 
 
 There is but one stratum of this rock in the region of the 
 map, of sufficient extent to render it necessary to delineate it. 
 I have sometimes noticed on the east side of Connecticut 
 river a kind of talco-micaceous slate: but not in abundance, 
 and rarely in place. I have crossed the stratum which is 
 colored on the map in Whitingham, Vt. where it is not less 
 than a mile and a half in width. I have traversed it also ia 
 flawley and Plainfield, and Professor Eaton says it extends 
 into Worthington — so that on his authority I have extended 
 it thither. The rock is of a much lighter color than mica 
 slate. At a distance, indeed, it has the aspect of gneiss. 
 The talc is nearly while, though sometimes of a light green, 
 and it contains a large proportion of silex. The strata are 
 but little undulating and nearly perpendicular, leaning a few 
 degrees to the west. On its east side, where it passes into 
 mica slate, an intermediate talco-micaceous rock is found, 
 containing numerous distinct crystals of black hornblende, 
 thrown in promiscuously, and exhibiting the most elegant 
 specimens. One variety has a ground that is green; anoth- 
 er has a white ground, and the contrast between these and 
 the imbedded crystals is striking. Large slabs of this rock 
 may easily be obtained; and if it will admit of a polish, it 
 would certainly be a beautiful addition to those marbles and 
 porphyries that are wrought for ornamental purposes. The 
 varieties of this rock aiay be . seen in any direction a few 
 rnds from iho meolina; house in Hawlcy: as likewise many
 
 Geology, i^-c. of the Connecticut. 27 
 
 other singular and curious aggregates which T have never 
 seen at any other place. Among these is sienitic porphy- 
 ry — and sometimes the talco-micaceous rock has its surface 
 covered with dehcate fascicular groups of hornblende. 
 
 The micaceous iron ore occurs in the talcose slate, and I 
 have never seen any of this sort of ore in any cabinet that 
 will compare at all for beauty with that in Hawley. 
 
 6. Chlorite Slate. Cleaveland. 
 
 Uncolored, but doited with black. 
 
 In the region under description,! know of but two deposits 
 of this rock of sufficient extent to be marked on the map; viz. 
 at West-Haven and IMilford* and in Whitingham, Vt. At 
 the former place it is but imperfectly characterised, espe- 
 cially at its Northern extremity. As we approach the 
 coast, in West-Haven, its characters become more decided, 
 and here we find numerous small crystals of octahedral 
 magnetic iron ore disseminated through it. Where the 
 cliffs of this slate have long been buffeted by the waves of 
 the ocean, these crystals have been worn out, and are de- 
 posited in large quantities, in the form of iron sand, on the 
 beach. On the east side of \&s*t-Haven harbour, at the 
 Light House, also, this sand appears in equal abundance — 
 and tons of it may easily be collected. On that side of the 
 harbour there is no chlorite slate; and whether the iron 
 sand found there is the remnant of former chloritic strata 
 now wholly disintegrated, or whether it is washed up from 
 the bottom of the Sound, where these rocks doubtless exist, 
 remains problematical. The latter supposition, however, 
 seems most probable. 
 
 The chlorite slate of West-Haven is extremely tortuous 
 and undulating, and is traversed by numerous irregular seams 
 of white quartz- It alternates with greenstone slate and 
 passes into it; and also with mica slate. These three rocks 
 are often so blended together that the distinctive characters 
 of each are lost. And as we approach the strata of the 
 Verd Antique, they seem to embrace also some of the prop- 
 
 ♦West-IIaven and a part of Milford have recently been incorporated in- 
 to a separate town by the name of Ariaasi. ^>-a>-z$,£_
 
 ^23 Geology, (^'c. of the Co7ineclicul. 
 
 eriies of this, and often to pass into it. Hence it is no easy 
 matter, in many instances, to give a name to the Milford 
 slate rocks, and the ahernalions above named, and also 
 with unstratified primitive greenstone, are numerous — so 
 that it was not possible in coloring the map to give to each 
 of these rocks the precise situation which they occupy on 
 the surface. 
 
 The direction of the chlorite slate strata, of which we 
 have been speaking, is from north-east to south-west. They 
 dip to the south-east, and their angle of depression below 
 the horizon rarely exceeds 30°. Sometimes, however, it is 
 90'. I think it will be found that the rocks of Woodbridge 
 and Mi ford pass laterally into one another. Thus, the 
 chlorite slate at i;s northern extremity is usually somewhat 
 talcose in its appearance, approaching to argillite, and as 
 you pass south, its characters continue to he more and more 
 developed.* 
 
 The chlorite slate colored in Whitingham, is the best 
 ;... characterised I have ever seen in New-England. It seems 
 ^ to be nearly pure chlorite, yet distinctly stratified, the lay- 
 ers being nearly perpendicular, leaning, however, a few de- 
 grees to the west. I know but little concerning the extent 
 of this stratum. Where I have crossed it, it was less than 
 half a mile in width. I have given it a place principally to 
 excite an attention to it. 
 
 T'his rock also occurs in beds in argillite in Guilford, Vt. 
 but they are not extensive. 
 
 7. SiENiTE. Cleveland. 
 
 Colored Gamboge Yelloiv, and crossed by oblique parallel 
 black lines. 
 
 This rock is marked in three places on the map. The 
 first is in Whateley and of very small extent — the second 
 extends from Whately to the south part of Northamptt3n ; 
 and the third is in Belchertown and Ludlow. The rock in 
 the two last places is very much alike, being for the most 
 part a kind of sienitic granite. In the first mentioned lo- 
 cality the rock is considerably different from that in the oth- 
 
 *! am indebted to Prof. Sillimau for this suggestion.
 
 Geology, cj-c. of the Connecticut, 2% 
 
 ers. I shall confine my remnrks principally to that range 
 extending from Whateiy to Northampton, because I have 
 examined this most. 
 
 As above remarked, this range appears to be mostly a si- 
 enitic granite, that is, a modification of granite; and very 
 different from that sienite which is associated with gray- 
 wacke and greenstone. A person coming from the west or 
 north-west towards the village of Northampton, will pass 
 over the most decided granite, associated with mica slate, 
 till he comes within four or five miles of that place. He 
 will then find the texture of the rock to be finer, and in some 
 instances it contains a portion of hornblende, while the pro- 
 portion of quartz is somewhat diminished, the felspar 
 frequently becomes red. Veins of graphic and common 
 granite, epidote, he. are more numerous, and the rock ap- 
 pears more disintegrated than the coarse grained granite. 
 In one part of a mass of this rock, may frequently be ob- 
 served a considerable proportion of hornblende, thus giving 
 the rock a sienitic aspect, while in another part, only a few 
 feet distant, this mineral is wholly wanting. Coming near- 
 er Northampton, however, we find the hornblende more 
 and more abundant, until we arrive at the eastern edge of 
 the range, where we find a rock containinglittle else than fel- 
 spar and hornblende, forming a real sienite. I have never yet 
 seen a specimen, however, in which careful inspection could 
 not discover both mica and quartz. The felspar is usually 
 deep flesh colored, and the hornblende sometimes black 
 and sometimes green. On the eastern border of this range, 
 especially about two miles north of the village of Northamp- 
 ton, on the west side of the stage road, this sienite assumes 
 a trappose and somewhat columnar form, both among the 
 loose masses and those in place.* Among the debris, the 
 three sided pyramidal form is most frequent; sometimes we 
 find a three sided prism, and sometimes, both among the 
 loose masses and those in place, two, three or four faces of a 
 prism of a greater number of sides. 
 
 Another spot for observing some interesting facts in re- 
 gard to this rock, is the south part of Whateiy. Two miles 
 south of the congregational meeting-house, on the road to 
 
 *This fact was first mentioned to me bv thr\t indcfatizable and able natu 
 talist, Mr. Thomas Nuttall.
 
 '30 Geology, «i'C. of the Connecticut. 
 
 Hatfield, is a manufactory of common earthen ware, and 
 here a small stream, running east, has cut across the great- 
 er part of the sienite range, and laid the rock bare nearly 
 the whole distance, which does not much exceed half a 
 mile. Let a person follow up the south side of this stream, 
 and in some of the ledges he will perceive a distinct strati- 
 fication of the sienite, though of little extent; one part of 
 the same ledge being often stratified and the other amor- 
 phous. In this place he will see, also, numerous intersec- 
 tions of granitic and other veins by which apart of the rock 
 has been displaced. In one of the ledges a little distance 
 from this stream, on the south side of a pond, may be seen 
 the prototype of Fig. 6. 
 
 Another interesting fact may be noticed in the sienitic 
 granite along this stream, especially on the northern side, 
 Bear the earthen ware manufactory. The rock here contains 
 numerous imbedded masses of other primitive rocks, as g?ieiss, 
 mica slate.quartz. hornblende, and a finer kind of sienite. And 
 what is peculiar, is that these imbedded fragments are almost 
 uniformly rounded — as much so as those contained in the 
 conglomerated rocks along the Connecticut; and they are 
 often so numerous that the rock appears like a real second- 
 ary conglomerate. The masses are very firmly fixed in the 
 base, and often there appears a mutual impregnation and 
 sometimes the veins of granite cut through the imbedded 
 fragments, as in Fig. 6. 
 
 Thus we have a real conglomerated sienite, and I had al- 
 most said a conglomerated granite : for much of the rock 
 containing these fragments is destitute of hornblende, while 
 all the ingredients of granite are present. And the instan- 
 ces in which this conglomerated rock occurs, are not confin- 
 ed to the particular locality above named — but it is to be 
 found in many other parts of the range. I have seen bowl- 
 ders of it in Surry, Alstead and Walpole in New-Hamp- 
 shire, but I did not there see the rock in place. 
 
 The Northampton sienitic range lies at a very low level. 
 A considerable part of it is hidden by a deposit of sand 
 through which it sometimes projects. The sienite in Bel- 
 chertown is also rather low. All the remarks above made, 
 in relation to the Northampton range, except that in regard 
 to its conglomerated character, will apply to this. The best 
 route which I have found for viewing this sienite, after cross*
 
 t 
 
 Geology, ^c. of the Connecticut. 31 
 
 iiig it in several places, is to pass by the right hand road from 
 Belchertown congregational meeting-house, to the meeting- 
 house in Ludlow. 
 
 The narrow deposite of sienite which is first mentioned 
 above, as occurring in Whately, is somewhat different in its 
 characters. Let the observer proceed northerly on the 
 main road from the congregational meeting house one mile, 
 till he comes to the farm of a Mr. Crafts. On the left hand 
 side of the road he will find a ledge of rocks which are 
 greenstone slate, nearly allied to hornblende slate, and some- 
 times to chlorite slate. TiCt him cross these strata westerly, 
 about fifty rods, and h#Brill come to a deposit of decided 
 unstratified primitive greenstone, about twenty rods wide. 
 Immediately succeeding this rock, he will find the sienite 
 above named. It consists of nearly equal proportions of 
 felspar and hornblende, the latter of a dark green and of a 
 distinctly crystalline structure; and the former white and 
 compact or very finely granular, entirely destitute of a foli- 
 ated structure, or pearly lustre. These ingredients seem 
 to be promiscuously blended, and the rock appears to be 
 peculiarly well adapted for being wrought and polished for 
 useful and ornamental purposes. The bed is not very ex- 
 tensive, only about six rods wide at the place above men- 
 tioned, and I have never been able to trace it more than one 
 or two miles. It is separated from the mica slate by a nar- 
 row stratum of greenstone slate. 
 
 Sienite, or sienitic granite, occurs in many other places 
 along the Connecticut; but in no other place have I found 
 it extensive enough to deserve a place on the map, except 
 perhaps in Chatham, and with the relative situation of this I 
 am not sufficiently well acquainted. Where I have crossed 
 it, it appeared to form a bed in porphyritic hornblende slate. 
 
 8. Primitive Greenstone. — Cleaveland. 
 
 Colored Carmine or Rose Red, and marked hy parallel lines 
 crossing each other. 
 
 This is one of Werner's varieties of primitive trap. If it 
 be asked what that is, I should suppose Mr. Maclure's supposi- 
 tion to be not an improbable one, that "what Werner calls 
 primitive trap may perhaps be compact hornblende ; or per-
 
 32 Geology, i^r. of the Connecticut, 
 
 haps the newest floetz trap when it happens to cover the 
 primitive." (Journal of Sci. Vol. I. p. 212.) Yet there are 
 two circumstances in regard to the rock here denominated 
 primitive greenstone, along the Connecticut, which have led 
 me to doubt its exact indentity with our newest floetz trap, 
 or secondary greenstone. 1. The primitive greenstone is 
 never amygdaloidal; while a great part of the secondary is 
 so. 2. The primitive greenstone not merely covers other 
 rocks, but forms beds in them. An example of this may 
 be seen one mile east of the Milford marble quarry on what 
 is called the old road leading to New-Haven ; where the > 
 
 greenstone lies between strata of aiiiil intermediate between >t>^ 
 greenstone slate and mica slate, and the rocks have every 
 appearance of being contemporaneous. 
 
 Primitive greenstone is colored in the following places on • 
 the map, viz. at West-Haven and Milford — at Wolcott — at 
 Whately, in the western part of Northfield and north part 
 of Gill. In regard to that in Wolcott, or the Eastern part 
 of Waterbury, I know but little, it being several years since 
 I observed it, and some snow being on the ground at'the 
 time. 1 put it down merely for the sake of pointing out its 
 locality. 
 
 The most extensive deposit of the rock is at West Haven 
 and Milford ; on both sides, but especially on the east side, 
 of the Verd Antique stratum. The hummocks of it that 
 appear very frequently, but irregularly, very much re- 
 semble the detached hills of secondary greenstone, except 
 that they are less elevated and the blocks of debris are usual- 
 ly larger. A little south of the Derby turnpike, this is the 
 first rock that shows itself as we ascend from the alluvial 
 plain of New-Haven on the Humphreysville turnpike alsOy 
 there is but a narrow stratum of chlorite slate separating it 
 from the alluvion. 
 
 This greenstone often becomes stratified on both sides of 
 the ridge, forming greenstone slate. At first, we perceive 
 a partial and interrupted stratification; and in a few feet it 
 becomes decided, extending through the whole mass. 
 There is also frequently seen a double stratification; one set 
 of planes crossing the other rectangularly or obliquely. Well 
 characterized greenstone slate, however, is not abundant in 
 Milford or West Haven. It usually soon passes into chlo- 
 ritic slate, or even into a bastard mica slate. An account ol
 
 Geology, fyc. of the Connecticut. 33 
 
 these slates has been long since given to the public by Prof. 
 Silliman in President Dwight's Statistical account of New- 
 Haven, page 11. Their strata run N. E. and S. W. and 
 dip to the S. E. The angle of depression below the 
 horizon rarely exceeding 30° or 40=". 
 
 Let hand specimens of this primitive greenstone and of the 
 secondary greenstone from East or West Rock be exhibited 
 to a geologist who had never visited the localities, and he 
 would not hesitate, I ihink, to pronounce that from East and 
 West Rock to be primitive, and the other to be secondary; 
 and for the reason, that he would find the secondary green- 
 stone to be much the coarsest and most crystalline. The 
 primitive greenstone of this locality is finely granular, and 
 agrees, in this respect, with Jameson's description of transi- 
 tion greenstone. Indeed, it has already been suggested (Jour- 
 nal of Science, Vol. 2. p. 165.) that the Verd Antique of Mil- 
 ford may possibly belong to a transition series ; and if so, this 
 greenstone, greenstone slate, and chlorite slate, and even 
 that bastard mica slate which is sometimes found between 
 this marble and the secondary, may belong to the same class. 
 The finely granular texture of transition greenstone, is how- 
 ever, by no means a distinctive character: since both the 
 primitive and floetz greenstones are described as possessing 
 the same. 
 
 The range of primitive greenstone in Northfield and Gill, 
 commences about two miles north of the northern termination 
 of secondary greenstone, and extends into Vernon. Its char- 
 acters are very similar to those of the same rock at Whately and 
 Milford. Some of it however approaches rather nearer the na- 
 ture of sienite: but still the hornblende predominates. It is of- 
 ten stratified and often semi-stratified, becoming greenstone 
 slate. Near the southern point I observed a vein or dike of 
 limpid quartz several rods long and one foot wide, traversing 
 this rock, having, a part of the distance, 5a«/6anJe5 of felspar. 
 The primitive greenstone occurring in Whately is some- 
 what different in its characters from that in Milford. It is 
 coarse and usually highly crystalline in its texture, being some- 
 times rendered almost porphyritic by the imbedded peif^es 
 of compact felspar, and sometimes being little else than pure 
 hornblende. It is not extensive and alternates m one in- 
 stance with sienite, the locality of which has been pointed 
 out in treatinc: of tlie latter rock.
 
 <34 Geology, ^c. of the Connecticut. 
 
 The greatest part of this greenstone is greenstone slate, 
 the strata having the same direction as that at Milford, and /> 
 being nearly perpendicular to the horizon, -kBeBring a few de-/*^** 
 grees one way or the other occasionally. This slate is als» 
 more crystalline than the same rock at New-Haven. It is 
 however a less degree of crystallization that chiefly distinguish- 
 es it from hornblende slate, towards which it verges and into 
 which it probably passes. Notwithstanding the very deci- 
 dedly fissile character of this slate, I have noticed in some 
 instances a tendency in it to the trappose form ; some of the 
 specimens having a cleavage, like many crystals, in two di- 
 rections, one coinciding with the direction of the strata and 
 the other running across the strata. The proportion of fel- 
 spar in this rock is small, often almost imperceptible. Chlo- 
 rite, however, abounds as in the greenstone slate of Milford; 
 and often it becomes real chlorite slate. Seams and beds 
 of quartz are common in the Whately rock and also granu- 
 lar epidote. 
 
 Some of the rock colored, as hornblende slate in Shel- 
 burne, he. much resembles certain varieties of this green- 
 stone slate ; and were the two rocks contiguous, it would be 
 difficult to draw the line between them. Indeed, by some, 
 this Whately rock would probably be denominated horn- 
 blende slate : but I think there is a distinction between the 
 two rocks; and so long as any of the stratified rocks of Mil- 
 ford retain the name of greenstone slate, it would seem the 
 Whately rock, from its resemblance and similar associations 
 with unstratified primitive greenstone, demands the same ap- 
 pellation. An observer will be struck with the resem- 
 blance of the greenstone strata at these two places, and with 
 their similar situation in regard to mica slate; and he will 
 be disposed to enquire whether these rocks were not once 
 continuous between these two places ; — and in the interme- 
 diate space, he will find sufficient evidence in the great quan- 
 tity of mingled detritus of other rocks, that the higher strata 
 have suflered much from some levelling agent in former 
 days.
 
 Geology, ^-c. of the Connecticut. 55 
 
 9. Argillite. 
 
 Colored Brick Red. 
 
 The remarks last made in regard to the primitive green- 
 stone, chlorite slate, &£C. will apply to this rock. For we find 
 it near the two terminations of the secondary tract and on the 
 same side of it— viz. in Woodbridge at the south end, and com- 
 mencing on the north at Leyden and extending at least as 
 far as Rockingham, Vermont. The northern deposite is 
 much the most extensive and is best characterized. In both 
 places, however, it is often tortuous and slightly undulating, 
 especially when passing into m.ica slate. It embraces nu- 
 merous beds and "tuberculous masses" of white quartz — 
 perhaps the milky quartz. The passage into mica slate is 
 usually very gradual, the characters of tlte argillite losing 
 themselves by imperceptible changes in those of the 
 mica slate, so that for a consiieurblc distance, the observer 
 may be in doubt to which ro; , co i'cier the aggregate. The 
 Woodbridge argillite occasionally alternates with mica slate, 
 (Journal Sci. Vol. 2. p. 203.) and I have ascertained that 
 this is the case also with that of Vermont. That which is 
 just beginning to pass into mica slate, alternates also with a 
 peculiar coarse limestone to be described under the next ar- 
 ticle; or rather, the limestone forms beds in the argillite — 
 for instance in Putney. 
 
 A principal object in extending the map so much beyond 
 the secondary region on the north, was to include all the 
 argillite to be found along the Connecticut. Whether I have 
 effected this object I am not certain. The Rev. E. D. 
 Andrews, who communicated to me several facts on this 
 subject, is of opinion that the northern limit of the argillite 
 is on the south side of Williams' river in Rockingham, three 
 miles north of Bellows Falls; but he had not examined the 
 regions beyond with sufficient care to decide the point with 
 certainty. 
 
 In Guilford, Vermont, this argillite alternates with a pecu- 
 liar rock which Professor Dewey remarks appears " to be 
 a talco-argillite with much quartz." Its stratification is less 
 perfect than the argillite ; or, rather, it has more of the ir- 
 regularities and tortuosities of m.ica slate. Its small extent
 
 3<> Geology, ^-c. of the Connecticut. 
 
 and imperfect characters prevented my putting it down as a 
 distinct rock. The stage road from Greenfield to Brattle- 
 borougli passes over it in the southern part of Guilford. At 
 the same place occurs well characterized chlorite slate ; but 
 not constituting any extensive rans;e. 
 
 One mile south of this spot, another rock occurs, which an 
 observer, at first sight, would pronounce to be granite. It 
 is unstratified* and has the color of granite; but seems to 
 be made up chiefly of quartz with a little mica interspersed. 
 It seems to be an aggregate to which no particular name has 
 as yet been applied; although the proportion of mica is so 
 small that it might almost be called quartz simply. It ap- 
 pears to form a large bed in argillite, or talco-argillite. 
 
 The strata of argillite, both in Connecticut and Vermont, 
 run in a direction nearly N. E. and S. W. and are highly in- 
 clined, generally varying but little from perpendicular. They 
 are undoubtedly primitive — that is, the evidence of this is as 
 great as in regard to the mica slate; both being highly inclined, 
 and destitute of organic remains. Indeed, Bakewell, who has 
 transferred argillite to the transition class, says " mica slate 
 has a near affinity to clay sVate ; and as I have arranged the 
 latter with rocks of the second class, it may perhaps be doubted 
 vi'hether mica slate should not also have been transferred to 
 the same class.'' (Geology p. 83.) Do we not here see to 
 what temptations the system maker is exposed, when pres- 
 sed with difficulties.^ However, as Professor Kidd remarks, 
 
 *" By stratification mc understand the divisions of a mass of rocks into 
 many parallel portions whose length and breadth greatly exceed their thick- 
 ness." Korlli-.fimcrican Rpv. JVo. 29, p. 232. 
 
 "Where a rock is stratified, is it necessarily bounded by parallel surfaces.' 
 If so, let us hear no more of inantle-sliaped, saddle-shaped, basin-shaped, 
 Irough-shappd siratification." Grecnongh^s Geology, Essay 1. 
 
 I would beg liberty to enquire, whether some of these difficulties might 
 not he removed by defining stratification to be the division of a mass of rock 
 into many parallel or fonfc«/rir portions.' But after all, tliis, like a thousand 
 other dpfniitions in natural history, is only an approximatian to the truth : 
 For if mathematical exactness be essential, we have never yet seen any rock 
 whose divisions were either parallel or concentric. BakeWelTs distinction 
 (Geology p. 31.) between "the structure which is caused by chemical agen- 
 cy, or by crystallization, and mechanical depositions," would perhaps give 
 relief to some of the difficulties in regard to stratification, were geologists 
 agreed what rocks have a structure caused by chemical Agency and what 
 ones are mechanical deposites. But they are not agreed on this point, as is 
 evident fiom the very example he brings to illustrate his principle, when 
 he says, that the division of slate rocks intolayers, is the result of their chem- 
 ical composition.
 
 Geology, Sfc. of the Connecticut. 37 
 
 it seems "the terms primitive and transition are daily be- 
 cominu' of less importance." 
 
 Quarries have been opened in the Woodbridge argillite 
 and it is employed in New-Haven for building. In V'er- 
 mont aiso, they have been wrought in Guilford, and Vernon, 
 two also in Dunimerston, S. E. of the centre of the town, two 
 in Putney, one and a half miles north of the meeting-house, 
 and one in Rockingham, a mile north of Bellows Falls. In 
 most of these the slate is of a good quality and easily ob- 
 tained; but at present they are not much wrought on ac- 
 count of the little demand for it, and consequent low price. 
 
 10. Limestone. 
 
 Granular Limestone, Eaton, Index, ^c. 
 
 Colored with India Ink. 
 
 This rock, in the country covered by the map, always 
 exists in beds in mica slate and argillite : never occu- 
 pying, however, so much as half the surface. I have co- 
 lored it in that region where it occurs most abundantly, 
 that is, in the mica slate nearest the argillite and the sand- 
 stone ; although its beds exist in nearly all the mica slate 
 north of Northampton on the west side of the river. It is 
 remarkably uniform in its appearance. Its exterior, when it 
 has long been exposed to the weather, is of a dark brown 
 color, showing more marks of decomposition than any 
 other rock in this region. The carbonate of lime is usual- 
 ly worn away at least an inch deep on the surface, and 
 the silex and mica are left in coarse grains, or warts, or in 
 projecting ridges. When newly broken the mica is uniform- 
 ly of a light gray, and the texture is coarsely granular and 
 dull, except the glimmering of scales of mica. The con- 
 stituents of the rock are carbonate of lime, mica and silex, 
 in somewhat variable proportions. In a specimen sent to 
 Prof. Dewey, he found about fifty per cent of carbonate of 
 lime and fifty of silex and mica. He judged that the silex 
 constituted about thirty five per cent and the mica fifteen : 
 and he judiciously adds, " the mica is in so great proportion, 
 you cannot call it silicious limestone. At least, ought it 
 not to be called a granitic aggregate, or silicious limestone 
 mixed with mica ?"
 
 38 Geology, &fc. of the Connecticut. 
 
 The beds of this rock vary in width from a few inches 
 to 20 feet, and they rarely exceed this. They are un- 
 stratified, are sometimes traversed by veins of quartz, or 
 more frequently granite, and sometimes the rock becomes 
 so mixed with the mica slate, as to form one of its constitu- 
 ent parts. Rhombic crystals of carbonate of lime, of a 
 yellowish brown color, and agreeing by goniometrical ad- 
 measurement with the primitive form, are found imbedded 
 in this limestone, and sometimes these are connected 
 with irregulnr masses of quartz, and larger plates of mica. 
 It forms, when blasted, a good stone for underpinning. I 
 bave never seen it along the Connecticut, except in the 
 mica slate at the northwest part of the map — noi^ in any 
 part of New-England, nor in any mineralogical cabinet, — 
 yet it seemed to deserve a place on the map, and a descrip- 
 tion. 
 
 1 1 . Verd Antique. — Cleaveland. 
 
 Ophicalce Veinet. Brongniart. 
 
 Colored blue, and marked with oblique parallel lines. 
 
 The rich and elegant marble obtained from this rock has 
 induced me to give it a place on the map, although its ex- 
 tent is very limited. It extends northerly from Milford 
 harbour, 9 or 10 miles, apparently terminating two miles 
 west of Yale College. It constitutes an extensive bed in 
 chlorite slate, with which it sometimes alternates. I am 
 inclined, however, to the opinion, that the slate lying im- 
 mediately contiguous to the Verd Antique, although not 
 well characterised, approaches nearest to greenstone 
 slate. Yet, decided chlorite slate, appears usually only a 
 few rods distant. In some places, the Verd Antique is a 
 quarter of a mile in width, and forms ledges of considera- 
 ble elevation and extent. It is stratified — the layers being 
 thick and parallel to the slate rock enclosing it. The grain 
 is fine ; the rock is traversed by veins of calcareous 
 spar, magnesian carbonate of lime, and asbestus; and 
 is associated with chromate of iron and magnetic oxide 
 of iron, diffused, more or less, through the entire body of 
 the marble, and forming dark spots and clouds. The ser- 
 pentine is twisted and entangled in the limestone in almost 
 every form, and the green color of the rock may in gene-
 
 Geology, «^c. of the Connecticut, 39 
 
 ral be imputed to oxid of chrome — sometimes to the pres- 
 ence of serpentine, colored however, probably by the 
 same oxid. 
 
 This rock has been extensively quarried in two places, 
 one in Milford, 7 miles from New-Haven, and the other 
 only 2i miles from the city. From these are obtaj.icd a 
 marble which vies for elegance with any in the world. In- 
 deed, in the extensive collection of marbles and porphy- 
 ries in Col. Gibbs' cabinet in Yale College, we appeal to 
 those who have seen them, whether any specimens exceed, 
 or even equal in beauty and richness the Verd Antique from 
 Milford. The varied clouding and shading of the gray, 
 or blue ground of this marble with white, black, green, or- 
 ange and gold yellow, indeed, with varieties of almost 
 every color of the prism, give it an elegance that can be 
 realized only by those who examine it. The working of 
 this marble is difficult and expensive, and it is earnestly 
 hoped that the patrician part of our community will 
 not, by resorting to Europe for marbles, which, to say the 
 least, are no more elegant than this, compel the proprie- 
 tors of these quarries to abandon the undertaking. Spe- 
 cimens of this marble may be seen in most of the dwel- 
 lings of the wealthy citizens of New-Haven; and many of 
 the monuments in the grave yard of that city, are of the 
 Verd Antique. Several chimney pieces of it may be seen 
 in the Capitol at Washington. 
 
 Most of these facts in relation to this rock, I derive from 
 the published accounts of it by Professor Silliman. (See 
 Cleaveland's Mineralogy under Gran. Limestone, Marble, 
 and Verd Antique, 2d Edit. Also, Journal Sci. vol. 2, p. 
 165.) A minute account of this interesting formation is 
 still wanting; and Mr. Silliman has promised it. (See 
 •Tour. Sci. vol. 2, p. 166.) 
 
 12. Old Red Sandstone. Werner, Cleaveland. 
 
 It is agreed I believe among Geologists who have ex- 
 amined this region, that an extensive deposite of this rock 
 exists along the Connecticut. (See Cleaveland's Mineralo- 
 gy, 2d Edit. p. 759. Eaton's Index 2d Edit. p. 207. Tour 
 between Hartford and Quebec, p. 21, andMaclure's Geol- 
 ogy of the United States.) It is probably the oldest se- 
 condary rock in this region; and generally lies beneatli all
 
 40 Geology, S^c. of the Connecticut. 
 
 the rest. So that it does not, I apprehend, occupy so much 
 of the surface, as is generally supposed. There is much 
 slaty sandstone, red and gray, and some of it very argilla- 
 ceous, found along this river, which does not appear to be 
 the old red sandstone of Werner ; but to be a different 
 formation, which I have denominated the Coal Formation ; 
 and which others have called gray wacke slate. I know of 
 no instance in which I am certain that decided old red 
 sandstone lies above the coal formation; although they 
 evidently pass into one another. This coal formation, 
 with the secondary greenstone and alluvion, occupies, I 
 should judge, nearly two thirds of the secondary tract 
 along the Connecticut; leaving not more than one third for 
 the old red sandstone. This rock occupies the greatest 
 extent of surface, as the map will show, in the vicinity of 
 New-Haven. Along the western side of the secondary, it 
 may be found all the distance, (occasionally covered by 
 alluvion,) from New-Haven to Bernardston, Mass. Yet, 
 it forms but few ridges or peaks of much altitude until we 
 come to the south part of Deerfield. There it rises ab- 
 ruptly from an alluvial plain in the form of the frustrum of 
 a cone, five hundred feet above the Connecticut; and the 
 peak is called Sugar Loaf; being but a few rods in diame- 
 ter at the top, and forming a striking feature in the scene- 
 ry of the country. This is the commencement of a range, 
 which, five miles north, rises 700 feet above the adjoining 
 plain, and then slopes to the north, almost disappearing in 
 Greenfield ; but rising again in the northern part of the 
 town and sending off one or two spurs into Gill. 
 
 The grain, even of the finest variety of this sandstone, 
 may be called coarse. Its colour is dark reddish, some- 
 times presenting spots or veins, of light gray, as in Hal- 
 field, Mass. Its cement is argillo-ferruginous, and the rock 
 usually exhales an argillaceous odour when breathed upon. 
 It contains a large quantity of light gray mica, the plates 
 being sometimes half an inch, or more, across, and insert- 
 ed promiscuously. This description applies to the finest 
 varieties of old red sandstone. But this passes into and 
 alternates With conglomerates of the same general charac- 
 terandof variousdegrees of coarseness. Theimbedded peb- 
 bles, vary in size from that of a musket ball to four or five 
 inches in diameter. They are usually quartz, felspar, graphic
 
 Geology, ^c. of the Connecticut. 41 
 
 and common granite, and rarely gneiss or mica slate. The 
 colorint^ matter of the rock, in most instances, has pene- 
 trated tlirough these pebbles, giving the graritic nodules 
 the same color as the rock, and the quartz a bluish as- 
 pect. This conglomerate frequently alternates with the 
 sandstone, and one half of the layer of a rock is sometimes 
 sandstone, and the other half conglomerate, no tissure be- 
 ing between them. Generally speaking, hov/ever, the 
 puddingstone increases in quantity and coarseness as we 
 ascend a mountain of this rock, and all the upper part of 
 the hill is sometimes composed of it. Probably more than 
 one half of the old red sandstone in the northern part of 
 the range is this conglomerate : yet, as it is evidently a 
 mere variety of the sandstone, it was thought aitogeth- 
 er unnecessary to attempt a division by different colors 
 on the map. 
 
 A considerable part of the range of this rock colored 
 on the east side of Connecticut river, i? somewhat dif- 
 ferent in its appearance from that I have been describing 
 on the other side. At least, there is one very abundant 
 variety that is not found on the west side. It consists of a 
 fine, siliceous, red sand, adhering together with but very 
 little visible cement. It has, however, an argillaceous 
 odour. The coherence is not as strong as in the coarser 
 sandstone, it being slightly friable. This rock may be seen 
 in place in the southwest corner of Ludlow, and the east 
 part of Long Meadow, Enfield, Somers, Ellington, kc. ; and 
 it forms a neater and handsomer building stone than any 
 other rock of the sandstone family which I have ever seen, 
 
 A part of this range of red sandstone, east of Connecti- 
 cut river, appears also to be verging towards the sandstone 
 constituting the coal formation. Examples of this may be 
 seen at the extensive quarry in Chatham, and also in Mid- 
 dletown — there seems to be a gradual passage of one 
 rock into the other — and the strata of both these r^^cks 
 have their dip in such a direction, as to lead one, at ^^=t' 
 to conclude that this old red sandstone lies above the c^^' 
 formation. The dip of both rocks is to the east. It do^s 
 not follow, however, from this circumstance, alone, th^*^ 
 the red sandstone does in fact repose on the other rock^* 
 Thus, let A B be a profile crossing the valley of the CcnneC 
 ticut. and exhibiting the strata of old red sandstone, havini; 
 
 6
 
 42 
 
 Geology, 4'C. of the Connecticut. 
 
 a dip as represented by the parallel lines. Let C D be a 
 deposite of the coal formation lying upon the old red sand- 
 stone, the strata of which have the same dip. Now, to 
 an observer passing along the surface from A to D, the red 
 sandstone, between A and C, appears to lie upon the coal 
 formation between C and D, whereas, the reverse is the 
 fact. This might apply to the rocks we are considering ia 
 Connecticut, were it not for what I think to be the fact, 
 (hat there is a gradual passage of the old red sandstone in- 
 to the coal formation. 
 
 
 These, and some other circumstances, made me suspi- 
 cious, for a time, that this range of sandstone east of Con- 
 necticut river, might not be the real old red sandstone, but 
 a member of the coal formation ; — and it was not till I had 
 traversed it the third time, that I felt entirely satisfied. 
 But much of it certainly does not differ, at all as I could 
 discern, from the old red sandstone on the western side of 
 the river; and we find likewise the very same conglome- 
 rate. The strata also, are of a similar thickness and dip, 
 varying as to the form, from six inches to two or three 
 feet; and as to the latter from 10° to 30° ; usually, how- 
 ever, not more than 10°. This dip, in all the red sand- 
 stone of the Connecticut, is below the eastern part of the 
 liorizon, with the single exception of a ledge that appears 
 in the west street of Hatfield, where the dip is to the 
 west. 
 
 This rock is extensively quarried for the purpose of 
 building, in almost every town along the river. Noble 
 specimens may be seen in the vestibules of the churches in 
 Ncw-Ilaven.
 
 Geology fyc, of the Connecticut, 43 
 
 Organic Remains. 
 
 These are very rare in our old red sandstone. I found, 
 however, in Deerfield mountain, one or two specimens that 
 belong to the petrifacta of Martin ; there being a perfect 
 substitution of a finer grained sandstone for the original 
 substance. I found only fragments, about four or five inches 
 long, and they appear to belong to the genus phylolite of 
 Gmelin's Linnaean System, and to the species lignite. 
 They are a third of an inch in diameter, and a little flat- 
 tened ; and seem to agree with Professor Eaton's descrip- 
 tion of certain petrifactions found in red sandstone on the 
 Catskill Mountain; (Index p. 211.) which he is inclined 
 to refer " to the tribe of naked Vermes.'' 
 
 Fossil Bones. 
 
 These occur in East Windsor, east parish, one hundred 
 rods south of Ketch's Mills. They belong to the conserva- 
 la of Martin, and, without much doubt, to the genus zooli- 
 ihus of Gmelin. The animal must have been about five 
 feet in length, and lay horizontally in the rock, eighteen 
 ieet below its top, and twenty-three below tbe surface of 
 the ground. The tail bone, as Dr. Porter, who lives near 
 the spot, informed me, projected beyond the general mass 
 containing the body of the skeleton, about eighteen inches 
 in a curvilinean direction. This, of which that gentleman 
 gave me a specimen, was easily distinguished by its nu- 
 merous articulations. On exposure to the air, the bones 
 begin to crumble and lose the appearance they presented 
 when first dug up, 
 
 'The-rock in which these bones were found, is decidedly 
 the old red sandstone. It agrees exactly with" that rock 
 as it exists at New-Haven, and to the distance of one hun- 
 dred miles north from that town. The rock enclosing the 
 bones is a little coarser than the finest varieties of this 
 rock, and in the rock above the bones, was found some 
 moderately coarse conglomerate. Whatever doubt I had 
 with regard to some other vari; lies of rock in that vicini- 
 ty, being the real old red sandstone, 1 could havo no 
 doubt in regard to this, after examining if.
 
 44 Geology, ^c. of the Connecticut, 
 
 13. Seco.\daky Greenstone. Cleaveland. 
 Colored Carmine, or Rose Red. 
 
 To ^ive the ranges of this rock, was one of the princi- 
 pal objects in constructing the accompanying map. For 
 although it be an anomalous, it is a highly interesting 
 fcrmation. The high mural precipices that almost uni- 
 versally show their naked faces in the ridges and hil- 
 locks of this rock — the immense quantity of debris that 
 frequentl}' slope up half, or two thirds the distance to 
 their summits — and the thin tufts of trees that crown their 
 tops, form much of the peculiar scenery of the Connecti- 
 cut. They remind the European of the basaltic and 
 other trap ridges of Scotland, Ireland, Saxony, Auvergne, 
 Italy, &LC. 
 
 In regard to the greenstone* north of Hartford, I feel 
 confident that every range of it to be found in place, is in- 
 serted on the map. South of Hartford some small and low 
 hillocks of it may have been overlooked, notwithstand- 
 ing all the assistance I have received from Prof. Silliman 
 and Dr. Percival. For, in some places, this rock seems to 
 be but a few feet in thickness above the sandstones, and to 
 be less continuous than in the northern part of the map. 
 In East-Haven and Branford especially, there are so many 
 ridges of greenstone, and these so irregular, that it is diffi- 
 cuk, on a map of such a scale, to make them all distinct 
 and accurate.! 
 
 The most southerly point of greenstone on the map is 
 the bluff in East-Haven, which fronts Long Island Sound, 
 and is about one mile and an half north of the Light-House. 
 The most northerly points of this rock are in Gill, auJ'Jii . 
 Ti^ lji|r w- The greenstone which occurs in the upper 
 part of Northfield, is more crystalline and of a coarser tex- 
 ture than in the intermediate distance, and is undoubtedly 
 
 * Trt save room, I shall omit, in the remainder of this article, the term 
 secondary, as applied at the head of the article. 
 
 t There oii?;ht to be a geolosfical map of the regfion about New-Haven, 
 on a larger scale than the one I have given : and we could name more thaa 
 one geutleinaa in that city, wlio is amply quMlitieJ for its construction.
 
 Geology, ^t- of the Connecticut. 45 
 
 primitive greenstone. Some of the specimens scarcely 
 differ from pure hornblende. 
 
 Between the two extremities of granite above named, 
 there i? not a mile, except in Amherst, where this rock ma_y 
 not be found in some part of the valley of the Connecticut 
 The most continuous and lofty ridge is that of which West- 
 Rock may be considered as the southern termination — al- 
 though the west rock range is broken off a few miles be- 
 tween Mount Carmel and the Meriden or Berlin moun- 
 tains. This ridge from West-Rock to Cheshire, presses 
 hard upon the primitive rocks, often approaching the slate 
 within a few rods. It presents, on the west, a lofty naked 
 wall, appearing as if nature had erected this mighty ram- 
 part to guard the secondary region of the Connecticut 
 from the encroachments of the primitive ; while the 
 great quantity of broken fragments along its base and scat- 
 tered in abundance for four or five miles over the chlo- 
 rite slate and argillite, evince that these ridges *•©#' 
 greenstone were once much more elevated than at 
 present. This range divides in the northern part of 
 Hamden, the eastern branch forming Mount Carmel, and 
 the western branch continuing into Southington, where it 
 chiefly disappears, although immense bowlders of green- 
 stone are scattered over the surface until we come to the 
 north part of Farmington. Here the ridge again commen- 
 ces, and inclining considerably to the right, terminates in 
 the north-east corner of Granby, Connecticut, in the Meni- 
 tick or Manitick mountain, on the top of which runs the 
 line between Granby and Suftield. 
 
 Mount Carmel terminates a little east of north from New- 
 Haven, and until we reach the Meriden or Berlin mountains, 
 thegreen«tone disappears. Commencing with these moun- 
 tains,we find an almost uninterrupted ridge ofgreenstone, con- - 
 tinning into Massachusetts. Its elevation decreases, for the- ^ 
 most part, as we go north, until we come to East-Hampton, 
 when it suddenly rises, like the coil of a huge serpent, and 
 forms Mount Tom, probably the highest point in the green- 
 stone ranges of New-England. I do not know that its 
 height has ever been accurately measured: but, comparinj? 
 it with Holyoke, it cannot be much less than a thousand 
 feet above Connecticut river. Connccticnt river crosses
 
 46 Geology, ^-c. of the Connecticut. 
 
 this range at the north end of Mount Tom, and on the op- 
 posite bank it rises again precipitously and forms Mount 
 Holyoke. This I found, with a nice sextant, to be eight 
 hundred and thirty feet above Connecticut river. North 
 of Holyoke the greenstone is curved towards the right and 
 continues of nearly the same elevation until it terminates 
 near the north-west corner of Belchertown, having reach- 
 ed the primitive region. 
 
 Nine or ten miles north-westerly from this point, we find 
 a narrow ridge of greenstone commencing, and pursuing a 
 course considerably west of north, it passes through Sun- 
 derland, crosses Connecticut river, runs through Deerfield, 
 crosses Deerfield river, and extending through a part of 
 Greenfield, terminates at the falls in Connecticut river. A 
 few rod? east of this termination another range commenc- 
 es and runs east of north through Gill, with some interrup- 
 tions, till it reaches its extreme northern point -Befitei^- 
 "firiri, two miles south of the primitive greenstone. 
 
 It will be seen by the map, that these greenstone ridges 
 separate the old red sandstone from the coal formation 
 nearly the whole distance from Berlin to Northfield; and 
 the rocks of the coal formation are frequently found lying 
 above the greenstone. The range oi green stone in Sun- 
 derland is very narrow, and being in an unfrequented spot 
 along the western margin of Mouni Toby, it was a long time 
 before I discovered its existence. Having once found it, 
 however, it was traced, without much difficulty, except 
 what an almost impassable precipice presented. It is from 
 ten to eighty rods wide. As you ascend the mountain from 
 the west, you first pass over a formation of old red sand- 
 stone, which is here a coarse pudding-stone. Next you 
 come upon the greenstone, most of which is amygdaloidal, 
 and is, so far as hand specimens will enable us to decide, 
 the real toad stone of Derbyshire. Immediately east ol 
 the green-stone you find the coarse, brownish red, and the 
 fine, fissile, argillaceous, gray and red sandstone slates of 
 the coal formation. These uniformly rise in higher ledges 
 than the greenstone; even one hundred or one hundred 
 and fifty feet above it. As you pass along in the direction 
 of the greenstone ridge, these precipices are not more than 
 ten feet from you on one hand, and the greenstone at no
 
 Geology^ Sfc. of the Connecticut. 47 
 
 greater distance on the other. The broken fragments of 
 the two rocks are confusedly mingled together, the sand- 
 stone breaking into large tables, and the greenstone into 
 pieces only a few inches across. These huge tables are 
 covered and fringed with a great variety of cryptogamous 
 plants, such as various species of Pamelia, Juggermannia, 
 Sticta, Collema, Bartramia, Hypnum, Polypodium, Aspidium^ 
 Aspknum, S/c. ; most of which are evergreen. And if the 
 geologist be also a lover of this department of botany, he 
 will find the wild and confused blending of such a variety of 
 interesting objects to repay him amply for tl>e labor and 
 even danger of clambering over the fragments. I have 
 never seen any rocks that seemed so congenial to the 
 growth of cryptogamous plants as those constituting Mount 
 Toby. 
 
 But to return from this digression. As the observer fol- 
 lows this greenstone southerly, commencing at its northern 
 extremity on the banks of Connecticut river, and sees the 
 lofty precipices of sandstone overhanging it, little doubt 
 will remain in his mind that the greenstone actually passes 
 under the sandstone. Yet any one acquainted with the 
 anomalies of trap rocks will have the question arising in 
 his mind, may not this greenstone, after all, here constitute 
 an extensive dike? and he will hardly be satisfied until he 
 sees the actual contact of the two rocks in place. One 
 mile north-east of Sunderland meeting-house, the greater 
 part of the greenstone ridge disappears and seems to run 
 under the sandstone; but here a {ew feet of debris hide the 
 actual junction. A little farther couth an actual junction 
 is seen; but the huge table of sandstone resting on the trap 
 is removed a iew feet from its original position. And, in- 
 deed, I never knev/ expectation so frequently disappointed, 
 just at the moment when it seemed about to be realized, as 
 in examining this range. It seems as if nature intended here 
 to teach the geologist a lesson of patience. But, at length, 
 one mile and a half south-east of Sunderland meeting- 
 house, the observer comes to a valley worn by a brook, 
 where finding the greenstone, which thus far has preserved 
 almost a right line, widening towards the east, and form- 
 ing a reentering angle in the sandstone, the angular 
 point being in the brook; he will have little doubt that
 
 48 Geology, ^'C. of the Connecticut. 
 
 the greenstone is here disclosed by the abrasion of 
 the superincumbent sandstone — ^and on following the 
 line of junction a few rods on the south side of the 
 brook, he will find the sandstone in place lying directly on 
 the greenstone, also in place. To one who has been accus- 
 tomed to see this latter rock mounting above every other 
 and monopolizing so muchspace forits broken fragments, it 
 must be gratifying to see it at last pressed down by a supe- 
 rior stratum, and buried by the debris of a higher rock. In 
 two places south of the point above described, other brooks 
 have worn away the sandstone, and the greenstone forms 
 in it a like reentering angle ; but the actual contact of the 
 rocks is hidden. 
 
 But Sunderland is not, after all, the best spot for observ- 
 ing the rocks of the coal formation lying above the green- 
 stone. I have been thus particular in describing the range 
 of greenstone in that place, rather to exhibit the difficulties 
 and trials to which the geologist is subject in examining 
 the trap ranges of the Connecticut, than because it was 
 necessary for this particular purpose. 
 
 Let the observer follow the Sunderland greenstone ridge 
 northerly across Connecticut river into Deerfield, and he 
 will here find it widening and increasing in altitude, pre- 
 senting a mural precipice on the west, and a gradual slope 
 on the east. Where it cros3es Deerfield river it has every 
 appearance of a vast dyke : although the sandstone rocks 
 do not appear immediately in contact with it. From the 
 top of the greenstone to the bottom of the river is more 
 than two hundred feet. The range continues to the falls 
 in Gill, where, as before observed, it terminates, and is suc- 
 ceeded by the red sandstone or conglomerate. And here 
 would I mention another fact in regard to the greenstone 
 and rocks of the coal formation. The latter do not mere- 
 ly lie above the former, but ihty alternate xcith one another. 
 Let the observer pass round the northern termination of 
 the greenstone range first mentioned, and follow down a 
 small river called Fall river, to its mouth, and just at this 
 point he will see the fine-grained, red, fissile, argillaceous 
 sandstone of the coal formation, mounting up fifty feet upon 
 the back of the greenstone at an angle of forty-five degrees* 
 And if he follow down the west bank of the Connecticut
 
 Geology, S/c. of the Connecticut. 49 
 
 two miles, he will have repeated opportunities of observing 
 the same fact ; the river having worn away the rooks so as 
 to afford a fine chance for observation; Let him now re- 
 turn and cross the mouth of Fall river eastward, following 
 up the north bank of the Connecticut, and he will find 
 the same red slate, cropping out about fifteen rods, when he 
 will come to another ridge of greenstone, wno?er which the 
 slate passes. If he follows the junction of the rocks ob- 
 liquely up the hill, on the east side of Fall river, a hundred 
 rods in a northeasterly direction, he will observe the green- 
 stone lying upon the slate more distiiictly. Let him return 
 to the bank of the Connecticut, where the sandstone slate 
 passes under the greenstone, and he will observe them both 
 extending in the same manner into the stream. If he now 
 go eastward along the bank of the river, he will find green- 
 stone twenty rods, and then the same or nearly the same 
 slate, rising on the back of the greenstone at an an^le of 
 forty-five degrees. Thus will he have conclusive evidence 
 of the alternation of these rocks. This alternation, cross- 
 ing this same spot, is represented in the profile accompa- 
 nying the map. No. 8 is the first ridge of greenstone above 
 mentioned: No. 9 the sandstone slate, rising on its back: 
 No. 10 the second ridge of greenstone; and No. 11 the 
 second stratum of the slate. This second ridge of green- 
 stone, as already marked, extends northeasterly into Gill 
 and terminates Typ fhri ii ^'r ,«|t pflit—'^*^H ip*!'*'fi*^- ^^ ' 
 
 Another spot for observing the alternations of greenstone 
 and the coal formation is one hundred rods south-east of 
 Lyman's tavern, on the north-east side of Mount Tom, in 
 Northampton. A small stream here crosses the road, and 
 in its bed and banks several distinct beds of greenstone, 
 some of them not more than one or two inches thick, may 
 be observed at low water. 
 
 In the southern part of that extensive greenstone ridge ex- 
 tending from Amherst to Meriden, the sandstone of the 
 coal formation may often be seen on the west side of the 
 greenstone, lying underneath it. The shaft of the copper 
 mine at Newgate prison passes through the greenstone and 
 enters the sandstone: and Dr. Percival informs us (Jour. 
 Sci. Vol. 5, p. 42,) that in Southington, "sometimes the 
 sandstone can be very distinctly seen cropping out below 
 the greenstone on the west side of the ridges." At the 
 
 7
 
 50 
 
 Geology, ^c. of the Connecticut. 
 
 outlet of Salstonstall's pond in East-Haven, I have observed 
 a grey micaceous sandstone of the coal formation, passing 
 under tlie greenstone with a considerable dip; and also two 
 miles south of Durham village, on the side of the turnpike 
 leading to New-Haven. 
 
 Dr. Percival, who has examined most of the greenstone 
 ranges in Connecticut on foot, illustrates his views of the 
 relative position of this rock and the coal formation as fol- 
 lows — referring particularly to the vicinity of Berlin. As 
 you ascend the mountain ridges from the west, the lowest 
 lock you find, after leaving the alluvion, is the old red 
 sandstone, represented below by A. Above this lie the 
 argillaceous sandstones of the coal formation, represented 
 by B. The cap of the ridge C is greenstone; precipitous 
 on the west side, but gently sloping on the east. Passing 
 on we come to another stratum of the coal formation; as 
 D. Next, perhaps, siicceeds another ridge of greenstone, 
 E — similar to C; and on its back, we fmd again the coal 
 formation, F; And sometimes the cap of greenstone is in- 
 sulated, as G. 
 
 Sometimes we find the greenstone resting immediately 
 upon the old red sandstone, without the intervention of a 
 third rock ; as at East and West Rock near New-Haven. 
 
 From all that 1 have seen and learned concerning these 
 rocks, I feel therefore, warranted in concluding, that, as a 
 general fact, our greenstone alternates with, or forms beds 
 in, the peculiar rocks of the coal formation ; and it seems 
 very probable that both these repose upon the old red 
 sandstone. As the slates of the coal formation dip below 
 the eastern horizon, it would seem we are furnished with 
 the reason why the mural faces of the greenstone are almost 
 universally on the western side of the ranges. 
 
 When greenstone rests on the coal formation, the lower 
 part of the greenstone seems to consist of little else than a 
 greyish black, indurated, ferruginous clay. Perhaps even
 
 Geology, iS^c. of the Connectiait. 51 
 
 wacke* may be found lying between the greenstone and the 
 saiidstone, as at Gallows-Hill near Hartford, and on the 
 west side of the Berlin ranges of greenstone. Some of the 
 greenstone occurring in the dykes of this rock in old red 
 sandstone, has a similar aspect. At the junction of the 
 coal formation and greenstone below the falls in Gill, the 
 columnar tendency of the latter rock entirely disappears, 
 and for several feet, the greenstone is distinctly, though 
 somewhat irregularly, stratified; the strata being parallel 
 to the sandstone. This may be seen to most advantage at 
 very low water; and the same may be seen, though less 
 distinctly, along the whole eastern border of this range of 
 greenstone ; and something of it on the east side of all the 
 greenstone ranges along the Connecticut. It ought here 
 to be remarked, also, that (his rock appears quite diflferent 
 in its composition on the eastern side, especially of the 
 range passing through Deerfield and Greenfield. The in- 
 durated clay seems in a great measure to take the place of 
 the hornblende, and the basis of the rock has a wackelike 
 appearance. Much of it is amygdaloidal; but the imbed- 
 ded minerals are usually quite different. On the east side, 
 the most abundant is chlorite, having a radiated aspect, and 
 green earth ; whereas, on the west side, this is scarcely to 
 be found. The radiated zeolite on the west side is finely 
 fibrous; on the east side, the crystals are larger and trans- 
 parent, resembling the Thomsonite of Dumbarton in Scot- 
 land. The rock on the eastern side is, also, more decom- 
 posable than on the opposite side. 
 
 The eastern side of this rock is not, however, all amyg- 
 daloidal. Near where Deerfield river passes through the 
 range, on the north bank, this rock contains distinct crys- 
 tals, or rather plates of felspar; and thus becomes a porphy- 
 ritic greenstone. "It even approaches to ophites," says 
 Professor Dewey. The same rock contains good prehnite, 
 and in the prehnite may be found pyritous copper. 
 
 I should judge that about one half of the greenstone of 
 the Connecticut constitutes the base of amygdaloid, and 
 very much of it appears to be genuine toadstone. The cavi- 
 ties are usually spheroidal or almond shaped, sometimes 
 reniform, and frequently cylindric. Those of the latter 
 
 *I have recently found icacke perfectly well characterised, and very 
 abundant, at the foot of the very lofty mural precipices, two miles north 
 of Monte Video, on the Talcot mountain, ten miles VV, of Hartford. — Editor
 
 62 Geology, c^-c. of the Connecticut. 
 
 form are often a foot or more in length, and arranged par- 
 allel to one another; the rock appearing as if bored through 
 repeatedly by an augur. The imbedded minerals are cal- 
 careous spar, analcime, chlorite, quartz, chalcedony, chaba- 
 sie, zeolite, and Professor Silliman has recently discovered 
 gypsum* in a specimen sent him from Dr. Cooley ; a new 
 fact we believe in Geology, and one which renders it not 
 improbable that this valuable mineral may be found in abun- 
 dance along the Connecticut. 
 
 This amygdaloidal greenstone is probably most abundant 
 at the lower part of the greenstone ridges ; while the upper 
 part is solid and usually columnar. Frequently, however, 
 the columns are amygdaloidal to their top, and sometimes, 
 as in Deerfield, in passing in the direction of the ridge, you 
 will find alternate successions of amygdaloidal and solid 
 greenstone columns. On breaking into the interior of the 
 former, we often find them a rich reservoir of rare miner- 
 als. The cavities are usually small; but sometimes sever- 
 al inches in diameter, occupied by quartz and amethystine 
 geodes, or chalcedony, or agates, or a peculiar pseudo- 
 morphorus quartz to be described when we come to treat 
 of particular minerals. The largest and best agates occur 
 usually among the greenstone that is not much amygdaloid- 
 al. sometimes occupying a cavity, part of which is in one 
 coAumn and part in another. They are very frequent, and 
 Sf. M of those recently discovered by Dr. D. Cooley, in 
 Deerfield, are probably the finest yet found in this country. 
 A particular account of them will be given in the proper 
 place. Prehnite sometimes forms a thin incrustration on 
 the columns that are not amygdaloidal; and between the 
 ioinrs of those that are so, is sometimes interposed a thin 
 coatingof various minerals, among which epidote frequently 
 predominates. 
 
 Some of the amygdaloid is very vescicular, bearing some 
 resemblance to the slag of an iron furnace or lava. The 
 cavities, in certain rare varieties, are various in form ; and 
 the base is whitish brown, reddish, and even brick red ; 
 containing, in the cavities, much prehnite, and this mineral, 
 together with calcareous spar, seems, in some instances, to 
 be mixed with the greenstone to form the base. An en- 
 thusiastic Huttonian would doubtless be gratified to find 
 
 *This gypsum was perfectly fresh — crystalized — white, and retaining; its 
 water of crystalization. — Editor.
 
 Geology, i^c. of tJie Connecticut, 53 
 
 such a variety. A locality of it may be found one hun- 
 dred rods north of the Deerfield river bridge in Deerfield. 
 at the western foot of the trap range. 
 
 The columnar tendency of our greenstone has often been 
 noticed. It may be seen in almost every ridge in a great- 
 er or less degree, on the mural face — and these columns 
 are sometimes remarkably regular. Good examples of them 
 occur on the south-west face of Mount Holyoke ; and still 
 better ones a mile east of the village of Deerfield, a quarter 
 of a mile north of the locality of chabasie,analcime,<kc. men- 
 tioned in the Jour, of Science Vol. 1. p. 115. They have 
 from three to six sides, are articulated, the points varying 
 from one to three feet in diameter, and of the same height, 
 exhibiting handsome convexities and corresponding concav- 
 ities. Haifa mile south of this spot may be seen columns 
 curving to the right and left as they ascend ; thus forming 
 a portion of an arch. The geologi>t, who traverses this 
 ridge, can hardly avoid traversing in imagination the giant's 
 causeway, StatTa and the Hebrides. 
 
 Some of the less perfect columns have a remarkably fis- 
 sile tendency ; forming good hand specimens of pseudo- 
 green-stone slate. Globular distinct concretions of this 
 rock are not unfrequent among the amygdaloid ; composed 
 of concentric coats of greater specific gravity than the rest 
 of the rock. I have noticed them in Deerfield, and on the 
 New-Haven turnpike between Durham and Northford, they 
 are abundant, and from two to twelve inches in diameter. 
 
 The general aspect of our greenstone, where it has been 
 long exposed to the weather, is reddish brown. When 
 newly broken it is greenish, often somewhat lively. Some- 
 times it is greyish black, and. very rarely, has the color 
 of a brick that has been burnt very hard. This variety is 
 compact and the felsparimperceptible. It is often the fact, 
 indeed, that the two ingredients in other varieties, are not 
 to be discovered by the naked eye. or with an ordinary lens. 
 
 A question then occurs, whether some of the varieties of 
 this rock are not genuine basalt ? Certainly some of them 
 answer the description of that rock, so far as external char- 
 acters are concerned, to say the least, as well as of green- 
 stone. And, indeed, if "greenstone and basalt may not 
 unfrequently be seen passing into each other in the 
 same stone, as D'Aubuisson and Dolomieu have observ- 
 ed," (Bakewell's Geology, p. 11 9.) there seems no rea-
 
 54 Geology, ci^c. of the Gonntcticut. 
 
 son to doubt that this fact may exist in this country as- 
 well as in Europe. Were I to refer to particular locaMties 
 for rocks resembling basalt, I should mention the foot of 
 Mount Tom on the north-east side, and a part of the range 
 passing through Deerfield. It would not surprise me, should 
 future geologists make a division of our greenstone, calling 
 a part of it basalt; dividing the upper part of theridges from 
 the lower, or the eastern side from the western, or both. 
 A geologist, to be able satisfactorily to make these divi- 
 sions, or to decide whether any of our rock is basalt, ought 
 to have traversed extensively and observed minutely the like 
 rocks in Europe ; and, therefore, I leave the subject to 
 abler hands. 
 
 A good locality for observing many of the varieties of 
 greenstone above described within a narrow compass, is on 
 the north bank of Deerfield river, about sixty rods from the 
 bridge. Let a person cross the bridge to the north, and 
 take the right hand road, until he comes to where the road 
 passes round the end of the greenstone ridge. Here he 
 will first see the most common variety, having a columnar 
 tendency ; and a few rods beyond, the reddish brown vari- 
 ety,* and in a wall, supporting the road on the right hand, 
 he will find abundance of the porphyritic greenstone, hav- 
 ing a somewhat stratified structure. Here, too, he will 
 find some specimens covered with a ferruginous coating ; 
 so much charged with iron, indeed, that efforts have been 
 made to smelt it. Indeed, a mass of four or five pounds 
 from almost any part of this greenstone range, when held 
 by the side of a compass, will move the needle. 
 
 It is not always the case, nor even generally, that the 
 greenstone ridges that are marked as continuous on the 
 map, are strictly so. They are often composed of numer- 
 ous peaks or ridges, partially detached, but yet constitu- 
 ting a single range when viewed at their bases. And some- 
 times, when there appears to an observer passing along the 
 western side of the range to be an uninterrupted wall, clos- 
 er examination will show, that it is made up of several dis- 
 tinct ridges, so lapping on upon each other, and so near one 
 another, that they appear continuous. The mural face of 
 the ridges and hillocks is usually on their western side ; 
 but sometimes on the opposite side, as in the high moun- 
 
 *I have a specimen of greenstone from a vein in Scotland resembling this, 
 except that the Scottish rock is much coarser.
 
 Geology, ^c. of the Connecticut. 55 
 
 tain between Durham and Northford ; and sometimes on 
 both sides, as Menitick mountain in Granby, Ct. Mount 
 Carmei in Hamden, and Mount Tom in East-Hampton, at 
 its southern extremity. The broken frau;ments of the green- 
 stone, of almost every shape, seldom of any regular figure, 
 and of various sizes, usually slope up more than half the 
 distance from the bottom to the top of the ledge. This 
 debris is highly interesting to the chronologist, because it 
 furnishes him with a decisive 
 
 Cosmogonical Chronometer. 
 
 Every one who lives in the vicinity of these greenstone 
 ridges knows, that every year adds to the loose masses at 
 their base, at the expense of the columns above. The wa- 
 ter infiltrated through the thin soil on their tops, finds its 
 way into the narrow seams between the columns, and there 
 freezes in the winter, and by its expansion, removes the 
 rock a little from its place. This operation is repeated, 
 year after year, and thus some part of the rock is pushed 
 so far over the precipice that its center of gravity falls 
 without the base, and it comes thundering down, usually 
 dividing into very many pieces. Sometimes, if the foot of 
 a column gives way in this manner, the whole column 
 above, perhaps twenty or thirty feet long, is precipita- 
 ted, like a glacier, on the loose rocks below. Sometimes 
 only one or two of the lower joints fall out, leaving the 
 principal part of the column suspended, the shuddering ob- 
 server can hardly tell by what. He will also see evidences 
 in very many places, both in the ledge above him and in 
 the ruins beneath them, of recent instances of this kind, yv '~7l 
 
 Indeed, in almost any place along these mural ^mIi^, two /P^^"^""^*^ 
 or three of the outer columns are easily removed by the 
 application of a lever, being loosened by the ice of preced- 
 ing winters.* 
 
 Now every one must see that this levelling work cannot 
 have been going on forever ; and when we consider how 
 
 *On tearing down some of these columns a few years since, during; the 
 winter, in search of chabasie, &c. I found the spaces between them occupi- 
 ed by an immense swarm of the common musquilo. Poor insects I it was 
 all over with them as soon as the avalanche thundered. The Hon. Elihu 
 Hoyt informs me he found a swarm of these creatures in the winter, in a 
 hollow tree.
 
 
 56 Geology, 4'c. of the Connecticut. 
 
 very considerable is the quantity of rock yearly detached, 
 and compare this with the whole annount of the debris, the 
 conclusion forces itself upon us that the period when this 
 process began could not have been vastly renriote ; in oth- 
 er words, that the earth has not existed in its present form 
 from eternity. Its precise age cannot, indeed, be deter- 
 mined by this chronometer ; but I have often thought that, 
 judging from this alone, we should be led to conclude that 
 Moses placed the date of the creation too far back, rather 
 than not far enough. 
 
 Greenstone Dykes in Old Red Sandstone. 
 
 Professor Silliman conducted me to an interesting locali- 
 ty of these in East-Haven. They occur on the main road 
 from New-Haven to East-Haven, less than half a mile from 
 Tomlinson's bridge. We measured their width, and that 
 of the intervening sandstone, as they appear on the north- 
 easterly side of the road. The road here passes over a 
 small eminence, and the bank, on the north side, in its high- 
 est part, is almost fifteen or twenty feet above the road. 
 The dykes, occurring at this place, are exhibited on the pro- 
 file accompanying the map; and are laid down from a scale 
 of fifty feet to an inch, with the intervening sandstone. In 
 describing them 1 shall begin at the north western extremity, 
 that is, at the point nearest New-Haven : but a person wish- 
 ing to find them, will do best to go first to the other end of 
 the profile ; because the dikes are there more distinct. 
 
 No. 1. (See Profile.) Old red sandstone, coarse and con- 
 taining pebbles so as to form a conglomerate. The dip of 
 ., the strata is from 6° to 10° below the eastern horizon. The 
 t. sandstdfc^**!'^ very similar throughout. 
 ^ No. 2. Greenstone dike, 4 feet thick. 
 
 No. 3. Sandstone, 114 feet. This distance was measur- 
 ed by pacing ; the other distance by a rule. 
 
 No. 4. Greenstone, one foot thick. 
 
 No. 5. Sandstone, 9 feet. 
 
 No. 6. Greenstone, 9 feet. 
 
 No. 7. Sandstone, 40 feet. 
 
 No. 8. Greenstone, 10 feet. The soil has so covered this 
 spot, and we having nothing with which to penetrate it, we 
 did not actually see the dike. But the walls are distinct,
 
 Geology, ^c. of the Connecticut. , 57 
 
 having small peices of the greenstone attached to them, and 
 exhibiting somewhat of an altered appearance, like the oth- 
 er walls, so that little doubt could remain of this being a gen- 
 uine dike. 
 
 No. 9. Sandstone, 52 feet. 
 
 No. 10. Greenstone, 5 feet. 
 
 No. 11. Sandstone, 45 feet. 
 
 No. 12. Greenstone, 10 feet. 
 
 No. 13. Sandstone, 19 feet. 
 
 No. 14. Greenstone, 7 feet. 
 
 No. 15. Sandstone, 7 feet. 
 
 No. 16. Greenstone, 4 feet. Here the greenstone is hid 
 by the soil as is also the sandstone at the other end of the 
 profile : so that by removing this, probably other dikes 
 might be discovered. 
 
 Thus we have eight dikes in a distance of 21 rods. Some 
 of them require a little attention to discover them ; but 
 most of them arc very distinct. Some of them we traced 
 several rods on both sides of the road, in a direction per- 
 pendicular to the profile. Their width is sometimes sud- 
 denly decreased, or increased, several inches, so as to form 
 shoulders. They are not exactly perpendicular, but lean a 
 iew degrees to the west; and thus they are made to form 
 an angle considerably obtuse on their eastern side with the 
 sandstone. The latter rock is often somewhat glazed, hav- 
 ing|a specular aspect at the place of junction with the green- 
 stone, and the two rocks are not unfrequently mutually im- 
 pregnated, for several inches, with each other's properties. 
 
 I did not notice that the dikes at this place dislocate the 
 strata of sandstone: but I paid little attention to this point. 
 
 Several dikes, similar to the above, (three at least,) occur 
 in the old red sandstone on the right hand side of the turn- 
 pike from New-Haven to Middletown, on the east margin of 
 the salt marsh lying east of East Rock. One of these Is 
 remarkably distinct, cutting through a precipice twenty or 
 thirty feet high, and maintaining an uniform width of about 
 a foot. This crosses the strata nearly at right angles; but 
 makes an angle with the horizon of about 45° dipping to the 
 south west. On its roof, or upper side, near the lower ex- 
 tremity, a part of the sandstone strata are thrown upwards 
 two or three feet ; and they are affected laterally about the 
 
 8
 
 58 Geoiogij, i^c. of tilt Connecticut. 
 
 same distance. The dike along with the sandstone appears 
 to pass under a bill of gieenstone. 
 
 On the same turnpike, a few rods north-easterly of North- 
 ford meeting-house, four or five dikes occur; but ihey are 
 so bidden by the soil as not to be particularly instructive. 
 Inpassiiigfrom Durham to New-Haven on the same road, the 
 first low ridge of greenstone, which we cross, exhibits some- 
 thing, which I was almost disposed to denominate a dike of 
 coarse pudding stone, of the coal formation, in greenstone. 
 Certainly, there appears a peculiar juxtaposition of the two 
 rocks; but probably they exist in beds. 
 
 Two or three miles north of the dikes of which a profile 
 is given, Dr. Percival found several others; and perhaps 
 ihey are a continuation of the same. He found one also on 
 the road from Farmington to Hartford in the rocks of the coal 
 formation. 
 
 The greenstone found in these dikes has usually the dark 
 compact aspect of basalt — resembling, however, much of 
 the greenstone found along the Connecticut. Yet it seems to 
 want the characteristics of greenstone, and specimens which I 
 collected from the most perfect dike above described, half a 
 mile east of East Rock, even approach towacke. This rock 
 gives an argillaceous odoiu", is of a greenish grey color, has 
 an uneven fracture, is dull, and much softer than common 
 greenstone ; so that it may be cut with a knife : — and on com- 
 parison with a specimen of pure wacke from Calton Hill, (Ed- 
 inburgh,) which was analyzed by Dr. V\ ebster, it does not ap- 
 pear to differ, except in its greater hardness and perhaps less 
 softness to the touch. I have little doubt that these dikes will 
 ere long be denominated basaltic dikes : but, for the reason 
 formerly alleged, I forbear to name them thus. They are 
 an interesting feature in our geology, and deserve more at- 
 tention ; and it is peculiarly fortunate that they should be 
 situated so near a geological school and the first mineral cab- 
 inet in our country. 
 
 Juxtaposition of Secondary Greenstone and Primitive Rocks. 
 
 The actual contact of these has never been observed 
 along the Connecticut; and I know of but three places 
 where there is a probability of finding the junction — viz. in 
 the northeast part of Belchertown, in East-Haven and Bran-
 
 Geology, <J-c. of the Connecticut. 59 
 
 ford, and in the east part of Woodbridge. So far as I have 
 examined these places, I have always found a valley ofgeest 
 between the rocks. But this is often very narrow; as for ex 
 ample half a mile west of Branford meeting-house, where 
 granitic ledges lie on one side of the road and a greenstone 
 ridge on the other. 'Further examination of this and 
 the other points mentioned above, might discover associa- 
 tions similar to those occurring in the Hebrides. 
 
 Origin of Greenstone. 
 
 Does the greenstone of the Connecticut afford evidence 
 in favour of the Wernerian or of the Huttonian theory of its 
 origin? Averse as I feel to taking a side in this controversy, 
 I cannot but say, that the man who maintains, in its length 
 and breadth, the original hypothesis of Werner in regard to 
 the aqueous deposition of trap, vt^ill find it for his interest, if 
 he wishes to keep clear of doubts, not to follow the example 
 of D'Aubuisson, by going forth to examine the greenstone 
 of this region, lest, like that geologist, he should be compel- 
 led, not only to abandon his theory, but to v/rite a book 
 against it. Indeed, when surveying particular portions of 
 this rock, I have sometimes thought Bakewell did not much 
 exaggerate when he said in regard to Werner's hypothesis, 
 that, "it is hardly possible for the human mind to invent a 
 system more repugnant to existing facts." 
 
 On the other hand, the Huttonian would doubtless have 
 his heart gladdened, and his faith strengthened by a survey 
 of the greater part of this rock. As he looked at the dikes 
 in the old red sandstone, he would almost see the melted 
 rock forcing its way through the fissures; and when he came 
 to the amygdaloidal, especially to that variety which resem- 
 bles lava, he might even be tempted to apply his thermom- 
 eter to it, in the suspicion that it was not yet quite cool. And 
 without doubt he would see many a volcanic crater on the 
 top of these ranges, where, with our dull eyes, we see only 
 a pond or a quagmire. Even the occurrence of this green- 
 stone in beds in sandstone would present no obstacle, since 
 the discoveries by Dr. Macculloch in the isle of Skye of 
 similar beds, of whin stone; concerning which he says, 
 "there are no instances but where the alternating beds of 
 trap detach veins or dikes from the lower to the upper beds;
 
 GO Geolngy, <^-c. of the Connecticut^ 
 
 or the trap, quitting the interval between two given beda 
 of limestone or sandstone, makes its way across the one 
 immediately above or below, and then proceeds with a reg- 
 ularity as great between some other pair of proximate 
 strata"* (Transac. Geol. Soc. Vols. 3 and 4.) 
 
 By treating the subject in this manner I mean no disre- 
 spect to any of the distinguished men who have adopt- 
 ed either side of this question. To President Cooper es- 
 pecially, who regards the greenstone of the Connecticut as 
 volcanic, I feel much indebted for the great mass of facts he 
 has collected on the subject. And were 1 to adopt any hypoth- 
 esis in regard to the origin of our greenstone, it would be one 
 not much different from his. But I confess myself somewhat 
 given to scepticism in regard to any general geological sys- 
 tem extant; and Greenough on the First Principles of Ge- 
 ology has not aided much to remove my doubts. These 
 systems have been productive of great good by spurring for- 
 ward geologists to the collection of facts with a rapidity al- 
 most unequalled in any other science. When these shall 
 be still farther accumulated, it is hoped and may be expect- 
 ed, that a second Werner will arise, who, having not merely 
 the rocks of Germany but of the whole world before him, 
 and following the inductive method of Bacon, will be able 
 to construct a system of geognosy that will stand, like the 
 Newtonian system of gravitation, on a foundation too firm to 
 be moved. Perhaps such a system, after all, will prove 
 to bean amalgamation of the theories of Werner and Hutton, 
 and those names, which now form the watch words of op- 
 posing ranks, may descend to posterity, engraven side by 
 side, in harmonious union, on the column that supports the 
 system. If geological enquiries are not tending to this point 
 we are much mistaken. 
 
 President Cooper was led from the profile inserted in the 
 first Vol. of the Journal of Science, page 105, to conclude, 
 the Deerfield greenstone to be a dike disrupting the old red 
 sandstone. No distinction is there made between the sand- 
 stone of the east and west range ; but since I have ascertain- 
 ed that on the one side is old red sandstone and on the oth- 
 
 * It is by no means improbable that similar connecting dikes may be 
 found between the greenstone beds along the Connecticut. In all the places 
 ■where I have examined these beds, circumstances were unfavourable for 
 discovering the dikes had they existed.
 
 Geology, ^-c. of the Connecticut. 61 
 
 er a sandstone of the coal formation, this greenstone must 
 be regarded as a bed between them.* 
 
 14. Coal Formation. 
 
 Vuridij of Psammile. Brongniart. 
 
 Grey Wacke Slate. Eaton. 
 
 Colored brown by Umber. 
 
 It has long been known to mineralogists that coal was 
 found along the Connecticut ; and I denominate the rocks 
 containing it the coal formation, simply because its beds 
 occur in them, and in no other rock; the old red sandstone 
 containing none at all, but lying beloio it. The coal forma- 
 tion embraces numerous varieties and sub-varieties of rocks, 
 most of which alternate with one another and the principal 
 of which are the following. 1. Greenstone. This strictly 
 belongs to this class because it alternates with the other va- 
 rieties and in Berlin contains coal. But there werp suffi- 
 cient reasons for giving it a separate color and description, 
 which it is unnecessary here to mention. 2. Trap. Tuff. 
 {Trap Breccia, Cleaveland.) This occurs on the east side of 
 Mount Tom on the w^est bank of Connecticut river, and ap- 
 pears to lie between other rocks of the coal formation and 
 the greenstone, and perhaps alternates with the greenstone ; 
 though I cannot say much as to its geological relations, as I 
 have but recently discovered the rock and have had little op- 
 portunity to examine it. It consists of rounded or angular 
 fragments of greenstone, quartz and sandstone, united by 
 a reddish brown abundant cement of comminuted and de- 
 composed sandstone, greenstone or wacke. Scales of mica 
 appear scattered in the rock which seem to have belonged to 
 the sandstone. It exhales an argillaceous odour, is difficult to 
 break, and is about of the hardness of old red sandstone. The 
 imbedded masses of greenstone are larger than the quartz 
 or sandstone. I noticed some, six, eight, and even twelve inch- 
 es across. Perhaps this rock is not the real trap tuff of Eu- 
 rope. If not, it certainly deserves the name of greenstone 
 conglomerate: although many of the imbedded masses and 
 
 * Some other corrections needed to be made in tlie essay accompanying 
 that profile and map. But as I intend to comprehend all that is important 
 in that paper in this Sketch, a particular specification of corrections seema 
 unnecessary.
 
 62 Geology, ^c. of the ConnecticuL 
 
 the greenstone in the vicinity very much resemble basalt. 
 The sandstone imbedded is that fine-grained argillaceous 
 variety next to be mentioned. 3. ^ red, very dssWe, friable, 
 argillaceorts sandstone. It generally contains small scales of mi- 
 ca and isabundantalmostevery where, frequently lying imme- 
 diately upon the greenstone and alternating with it and with ma- 
 ny other varieties of rock hereafter to be mentioned. 4. Jl 
 Gray Micaceous Sandstone Slale, not argillaceous, grit coarse, 
 very fissile, layers even, some varieties much resembling 
 mica slate, others containing vegetable remains. 5. A simi- 
 larslatc; but much finer, harder and the layers undulating. 6. 
 A slate approaching in appearance to shale, but very silicious, 
 harder and very fissile, layers straight, surface not smooth, 
 dark gray. 7. SAa/e, generally bituminous,veryfissile, frequent- 
 ly micaceous with and without Ichthyolites. 8. A slaty rock of 
 the aspect of shale, and sometimes much resembling coal, 
 dividing into numerous small pieces of irregular form, and 
 disintegrating when exposed to the air and moisture. At 
 the falls in Gill. 9. A slate made up chiefly of indurated 
 clay, sometimes micaceous, easily scratched by the finger nail, 
 liable to disintegration. Falls in Gill, and cave in Sunder- 
 land, not abundant. lO. A fragmented rock, the fragments 
 chiefly a reddish brown quartz, appearing as if burnt, ce- 
 ment silicious and apparently ferruginous, rock very hard, 
 and appearing almost like porphyry, unstratified, not abun- 
 dant. In Gill. 11. Gray pudding-stone, distinctly stratifi- 
 ed, layers from six inches to a foot thick. Imbedded nod- 
 ules, quartz, felspar and mica slate, rarely more than an inch 
 in diameter, but very abundant, cement same minerals com- 
 minuted. Island in the falls at Gill. 12. Reddish stratified 
 pudding-stone, coarser than the last, and scarcely differing 
 from the conglomerate accompanying the old red sandstone. 
 Mount Toby, Belchertown and Gran by. 13. Very coarse 
 dark gray pudding-stone, scarcely stratified. Imbedded 
 masses often very large, even a foot in diameter, and very 
 abundant, consisting chiefly of mica slate, argillite and chlo- 
 rite^slate; but containing quartz, hornblende, talcose slate, 
 and sometimes granite, cement the same rocks comminuted. 
 Gill, Montague, Mount Toby, and Durham. Most of the 
 preceding rocks are often found alternating with one anoth- 
 er. 14. Jl gray imperfect limestone, very silicious, in beds 
 in sandstone slate, not fetid, not abundant, Gill. 15. Fetid
 
 Geology^ ^c, of the Connecticut. 63 
 
 carbonate of lime. At Northford. I do not know its exact 
 relative situation. 16. ^Bituminous carbonate of lime, in tiie. 
 coal formation at Southington and Middletown. 
 
 In tiiis series of rocks, and in this only, has coal been 
 found along the Connecticut. It occurs at Durham, Mid- 
 dletown, Chatham, Southington, Berlin, Somers, Ellington, 
 Enfield, South Hadley, and Southampton. In most instan- 
 ces it is hi^ihly bituminous and burns freely. The seams of 
 it are usually quite thin, rarely exceeding an inch in thick- 
 ness, yet often they are numerous. In Berlin, the coal oc- 
 curs in greenstone in a vein of crystallized quartz. (Journal 
 of Science, Vol. 5, p. 44.) In Southington it is found in 
 shale — in Somers, Ellington and Suffield, in friable argillace- 
 ous slate, (No. 3 above) in Enfield, in beds in gray micaceous 
 sandstone; (No. 4. above) also in the same rock, ("granu- 
 lated schistose aggregate" of Eaton, vide Journal of Science. 
 Vol. 1. p. 136,) in the drift of the S. Hampton lead mine. 
 
 The Connecticut river, in its passage between the town? 
 of Gill and Montague, has cut through the coal formation, 
 except a single ridge of greenstone on the west, as may be seen 
 by referring to the map. Through a considerable part of this 
 distance, especially in the most in terestingpart,the bassetting 
 of the strata is completely laid bare; and I have annexed to 
 the map a profile of their order and dip, which I shall now 
 proceed to describe. It is a vertical section, crossing the 
 map at the falls in Gill and the strata nearly at right angles, 
 extending on the west to the western part of Shelburne, sd 
 as to include a few other rocks beside the coal formation, 
 and on the east, to the mouth of Miller's river. The chief 
 object of this profile is to give a better idea of the coal for- 
 mation than could be obtained by mere verbal description. 
 That part of it, therefore embracing those rocks, is put down 
 from a larger scale than the other parts, otherwise the nu- 
 merous alternations could not have been represented. Es- 
 pecially that part between No. 8 and 40, is laid down from 
 a larger scale than the rest of the coal formation, because 
 this is the most interesting part of it and most distinctly laid 
 bare on the north bank of the Connecticut, extending 
 from the falls to the high greenstone ridge 100 rods west of 
 it. This part was observed most attentively, and a quadrant 
 converted into a clinometer, was used for determining the 
 
 * Bituminous marl slate? — £rf
 
 64 Geology^ ^t'* of the, Cowieclkul. 
 
 dip. The distances were all estimated by the eye, but it is 
 presumed they will in general be found not far from the truth. 
 From No. I to 56, inclusive, the stratified rocks all dip to 
 the east, as is evident from the section. The Nos. included 
 in parenthesis, refer to the general descriptions of the rocks 
 of the coal formation in the beginning of the article. 
 
 No. 1. Horblende Slate — Strata highly inclined, often be- 
 coming an aggregate of hornblende, quartz and mica, having 
 a porphyritic aspect. 
 
 No. 2. Mica <S7flfe— Dip 20° to 30°, undulating and tor- 
 tuous, passing on the east into argillite. 
 
 No. 3. Limestone — In beds in mica slate, already descri- 
 bed in the preceding pages. Unstratified. 
 
 No. 4. Argillite— D\p 60° to 90°. The southern limit of 
 this rock hardly reaches the line of the section : but a mile or 
 two north, its relative position is as represented on the profile. 
 
 No. 5. Old Red Sandstone — With red conglomerate. Dip 
 usually asmuch as 20°,beinggreaterthanis usual for this rock. 
 
 No. 6. Alluvion — A swamp. 
 
 No. 7. Old Red Sandstone — Dip between 20° and 30°. 
 
 No. 8. Secondary Greenstone — It is probable this forms 
 a bed between the old red sandstone and the coal formation : 
 but the former rock is never seen passing; under it in this vi- 
 cinity ; and, therefore, it must not be thus represented on 
 the profile. Width about half a mile. On the eastern side it 
 has, for a few feet in width, somewhat of a stratified structure. 
 
 No. 9. Red, Fissile, Friable, Argillaceous, Sandstone, 
 Slate — (No. 3.) It is fine grained and often micaceous, of 
 the color of brick, is easily cut by a knife, yields an argilla- 
 ceous odour, has an undulating surface generally, and is liable 
 to disintegration. This is probably the most abundant of 
 the rocks of the coal formation; and it usually lies next to 
 tile greenstone and alternates with it. It is found over a 
 large extent of country on the east side of the greenstone 
 ridge, stretching from Amherst to Berlin; although in Con- 
 necticut it more frequently is wanting in the mica and its 
 surface is more uneven. It forms much of the flagging 
 stone in Hartford and exists in place a foot or two below the 
 surface in that city; though it seems here in some instances 
 to approach to the nature of shale. The surface of the lay- 
 ers often appears a little glazed and is sometimes traversed 
 by numerous little ridges a mere line in thicknes and of the
 
 Geology, ^/-c. of the Connecticut^ 6§ 
 
 oubstance of the rock, which I have sometimes suspected 
 might be petrifactions ; and perhaps they are so. When 
 this rock is disintegrated it forms an admirable material for 
 the construction of roads; a good example of which m^y be 
 seen In the road between Hartford and VVeathersfield 
 
 Where the profile crosses this rock, it has a dip of 45° ; 
 and as already observed under the article greenstone, it 
 here mounts upon the back of the greenstone forty or fifty 
 feet. If we follow the junction of these rocks southerly, on 
 the west bank of the Connecticut, we shall find the slate con- 
 forming to the irregularities of the greenstone, thus forming 
 saddle shaped strata. In some instances we notice a sudden 
 curve from this cause, of 90°. At the first copper mine we find 
 on passing down the river, a narrovvspur of the greenstone ex- 
 tends a short distance into the slate, and the vein of ore here 
 passes from the greenstone into slate. Haifa mile south of 
 this point we find the slate crossed obliquely to the direction 
 of the strata by parallel seams dividing it into strips from one 
 to six inches wide and often five feet long. Sometimes we find 
 in these divisions six sided prisms of quartz, lying partially 
 imbedded and exhibiting both terminations in great perfec- 
 tion. I have seen seams very narrow containing green car- 
 bonate of copper, the sides of the vein being beautifidly gla- 
 zed, having a highly specidar aspect, and forming the saal- 
 hande of the Germans. The width of the rock on the sec- 
 tion is about fifteen rods, extending across the mouth of Fall 
 river. 
 
 No. 10. Greenstone — (No. 1.) This has been already 
 described when treating of that rock. Thickness of the for- 
 mation, 20 rods. 
 
 No. 11. Same as No. 9. (No. 3.) Thickness of the stra- 
 tum, 6 rods, dip 45°. 
 
 No. 12. Red Slate — resembles the last, but is more mi- 
 caceous, is divisible into thinner laminse, the surface of which 
 is even, and the color is less red. A beautiful rock. Thick- 
 ness 6 fet't, dip 45°. 
 
 No. 13. Reddish micaceons sandstone-Somewlmt con^^ om- 
 eraled, the imbedded pebbles of quartz and flesh colored fel- 
 spar, small and rounded, less fissile than the last, layers 
 thicker. Thickness twelve feet, dip 40°. 
 
 No. 14. Same as No. 12. Thickness 15 feet, dip 40°. 
 
 No. 15. Same as No. 9. Thickness 15 rods, dip 40° 
 
 9
 
 6t) Geology, <^c. of the ConnecticuL 
 
 No. 16. Reddish gray, friable, argillaceous sandstone 
 slate — Irregular, tortuous, disintegrating at the surface, a lit- 
 tle micaceous, containing numerous small specks of carbon- 
 ate of copper, and appearing to be an imperfect copper ore- 
 Thickness 4 feet, dip 40° 
 
 No. 17. Hard, compact limestone — (No. 14.) Fracture 
 dull, containing a large proportion of silex, feebly efferves- 
 cing with the acids. Thickness of the stratum only a foot, 
 dip 48°, not divisible into layers This very imperfect and 
 small bed of limestone is the only locality of limestone rock 
 I have ever found in the secondary region north of Hartford. 
 
 No. IS. Gray, Micaceous sandstone slate — (No. 5.) Ir- 
 regular, tortuous and undulating, not as easily and as hand- 
 somely separating into layers as the red slate, resembling 
 some varieties of the mica slate, scarcely argillaceous. 
 Thickness 6 feet, dip 40°. 
 
 No. 19. Same as No. 9. Thickness 12 rods, dip, 43°. 
 
 No. 20. Coarse, reddish conglomerated sandstone — Con- 
 taining imbedded pebbles. Scarcely different from No. 13, 
 except somewhat coarser. Thickness 6 feet, dip 43°. 
 
 No. 21. Same as No. 12. Thickness 3 rods, dip 43°. 
 
 No. 22. Gray, micaceous, sandstone slate — Rough to the 
 touch, coarse, granular, scarcely argillaceous, not separating 
 into so thin layers as the red slates. Surface not undulating 
 or tortuous. Thickness 13 feet, dip 43°. An excellent flag- 
 ging stone. 
 
 No. 23. (No. 9.) Soft argillaceous slate — Surface smooth, 
 scarcely undulating, divisible into thin plates, easily scratch- 
 ed by the finger nail, and consisting of little else than clay 
 moderately indurated. Thickness 5 feet, dip 45°, easily 
 disintegrated, rarely micaceous. 
 
 No. 24. Gray micaceous sandstone slate — Similar to No. 
 22, but softer to the touch and finer grained, more undula- 
 ting and divisible into thinner layers, containing vegetable 
 remains converted into perfect coal. These were so numer- 
 ous in one spot, that I thought I had found a bed of coal. 
 Thickness 3 rods, dip 40°, 
 
 No. 25. Gecst—2 rods. 
 
 No. 26. Shale — Color very dark, containing sometimes 
 small scales of mica, surface a little knobby, containing 
 abundance of sulphuret of iron and spheroidal nodules from 
 half an inch to two inches diameter, oi argillaceous iron ore?
 
 Geology, ^c. of the Connecticut. 6? 
 
 very similar to the shale containing the ichthyolite at Sun- 
 derland. Thickness 1 rod, dip 40°. 
 
 No'. 27. Same as No. 24. 2 feet thick, dip 40.* 
 
 No. 28 A stratum of coarse grayish sandstone, or rather 
 conglomerate, 2 feet wide, dip 40°. 
 
 No. 29. Same as No. 24. Thickness 5 rods, dip 40°. 
 
 No. 30. Geest — 10 feet. It may be well, perhaps, here 
 to remark, that shale usually forms the roof and floor of coal 
 beds, and that this geest and that of No. 25 lie immediately 
 below shale. Connect this fact with another, " that the seams 
 or strata of coal rise up to the superficies of the globe as well 
 as all other strata, only they do not always push up so bold- 
 ly to the very surface of ihe ground as many hard stones 
 and other indurated strata are found to do ; for on account 
 of the tender and more friable texture of the coal, the super- 
 ficies of the stratum is often mouldered down and lies con- 
 cealed under a thicker or thinner bed or cover of clay, grav- 
 el, sand, or earth." (Williams Mineral Kingdom, Vol. 1. p. 
 13i5 2d edition.) If then coal can be found along the section 
 here described, (which I suspect to be quite doubtful,) the 
 best spots to search for it are Nos. 25 and 30. 
 
 No. 31. Shale — 10 feet thick, dip 40°, containing abun- 
 dance of nodules o^aritil/aceous iron ore ? Rock rather hard 
 for pure shale, not liable to much disintegration. 
 
 No. 32. Coarse, gray, sandstone or conglomerate — Rock 
 harsh to the touch, imbedded masses not large, layers thick. 
 Thickness two rods, dip 40°. 
 
 No. 33. Same as No 24. Thickness 3 rods, dip 43°. 
 
 No. 34. Shale — Alternating with, and passing into, a 
 bluish, gray, fine grained slate, harder than the shale, though 
 perhaps only a variety of it. A little micaceous. Thick- 
 ness 3 rods, dip 43°. 
 
 No. 34. Blackish gray slate — Similar to that mentioned 
 under the last No. but less fissile and much harder, indeed, 
 it breaks with nearly as much difficulty as greenstone, and 
 where it is worn by the water it somewhat resembles that 
 rock. For it contains numerous irregular cells, sometimes 
 two inches in diameter, formerly filled, probably with argilla- 
 ceous iron ore^ On breaking the rock it? structure is slaty 
 and it is a little micaceous. Thickness 2 feet, dip 40°. 
 
 No. 36. Coarse grayish sandstone or conglomerate — like 
 No. 32, layers 2 feet thick. Thickness 20 feet, dif» 40^
 
 t}8 Geology, i^'c. of (he Connecticut. 
 
 No. 37. Red slaie — As No. 9, but harder and coarser 
 and less irregular on the surface of the layers. Thickness 
 5 rods, dip 40^. 
 
 No. 38. Same as No. 22. Thickness 20 feet, dip 40*'. 
 Mo. 39. Similar to No. 38, hut more micaceous and di- 
 visible, into thinner layers; resembles much, certain varie- 
 ties of mica slate, except that the silex has a more earthy as- 
 pect. .But it would not be difficult to deceive almost any 
 geologist, by labelling hand specimens, mica slate. Thick- 
 ness 2 feet, dip 40°. 
 
 No. 40. Same as No 37. Thickness 10 feet, dip 40^ 
 This carries us to the dam across the Connecticut. 
 
 No. 41. Hard grai^ sandstone slat f — Like No. 22, but 
 more undulating and irregular. Thickness 5 rods, the 
 remaining distance the scale is much reduced. 
 
 No. 42. Very near No. 41, but coarser and not so undu- 
 lating. Thickness 8 rods. 
 
 No. 43. Coarse gniy conglomerated sandstone — layers 
 thick; Thickness 12 rods. 
 
 No. 44. Same as No. 40. 3 rods thick, dip 35°. 
 No. 45. Alluvion — 20 rods. 
 No. 46. Same as Mo. 32, about 2 rods thick. 
 No. 47. Same as No. 40, 1 rod thick. 
 No. 43. Alluvion — a quarter of a mile; beyond this the 
 section is continued on the south bank of the river. 
 No. 49. Same as No. 37, one half a mile. 
 No. 50. (No. 10.) A singular fragmented rock — unstrati- 
 fied, 20 feet thick, very hard and tough, imbedded frag- 
 ments, chiefly reddish brown quartz, appearing as if it had 
 imdecgone the action of fire, a little micaceous, cement often 
 blackish, appearing like veins, apparently ferruginous, rock 
 resembling some varieties of porphyry. 
 
 No. 51. (No. G.) Dark gray, very fissile sandstone slate — 
 Harder than shale, somewhat argillaceous in its odour, a lit- 
 tle micaceous, surface rough and grit coarse, slightly sono- 
 rous when struck, 1 rod thick, dip 40°. 
 No. 52. Same as No. 50, 1 rod thick. 
 No. oi. Similar to No. 39, 5 rods thick. 
 No. 54. Alluvion between half and three quarters of a 
 tnile. 
 
 No. 55. Same as No. 9, half a mile.
 
 Geology, ^'C. of the Connecticut. 6,9 
 
 No. 56. Same as No. 51, extending nearly a mile, dip 
 at first 35°, but gradually decreasing to 15°. • The direction 
 of the strata of this rock is quite different from the other va- 
 rieties, which generally have a direction between north and 
 northeast. But this variety is so much wheeled that it runs 
 not far from east and west; and in passing up the river we 
 sail for a time nearly parallel to the direction of the strata. 
 I do not see why this rock might not be employed for roof- 
 ing ; and if so, the situation of the quarries would surely be 
 very advantageous. 
 
 No. 57. Same as No. 9, strata nearly perpendicular, but 
 leaning a little to the east, and their direction nearly the 
 same as that of all the varieties mentioned except ihe last. 
 Thickness 10 rods. 
 
 No. 58. (No. 8.) Blackish tortuous slate — Stratification ir- 
 regular and the layers dividing into numerous shapeless pie- 
 ces by fissures in every direction. The surface of these 
 amorphous pieces is frequently a little glazed. Rock, friable, , 
 scarcely micaceous, argillaceous, s:rata leaning a few degrees 
 to the east, 20 rods thick. This rock forms a bed at the island 
 in the falls in the Connecticut three miles below this spot, 
 and there it is exposed to the occasional action of the water 
 and is disintegrated so as to leave the superincumbent 
 strata projecting over it several leet, and it very much re- 
 sembles impure coal : but I could not determine that it con- 
 tains any. It is probably a variety of shale. 
 
 No. 59. Very coctrse, dark gray puddingstone — A gene- 
 ral description of this rock has already been given in the be- 
 ginning of this article. (No. 13.) Imperfectly stratified at 
 this place, rather harder than the old red sandstone conglom- 
 erate, yet appearing as if composed of little else than a mass 
 of pebbles, the cement bein^; not abundant, extending at 
 least a quarter of a mile. The Connecticut at this place 
 has worn a passage between this rock and the primitive, and 
 high ledges appear on both sides of the river, which, on 
 comparison, seem to differ almost toto coelo. The pudding- 
 stone extends through Montague, sometimes assuming a 
 reddish aspect, and in Sunderland forms a considerable part 
 of Mount Toby. Here it alternates with the red and gray 
 slates above described; and it is curious to observe the fre- 
 quent sudden changes from this coarsest of conglomerates t» 
 fine grained slates. ^ff
 
 70 Geology^ fyc. of the Connecticut. 
 
 Where the profile crosses this rock, some of the imbed- 
 ded massos appear at their surface as if they had undergone 
 the action of fire. On breaking a mass of gray quartz con- 
 taining a little mica, a zone of half an inch wide appeared at 
 the outer edge, of a brick colour, indicating a chemical 
 change either by fire or water, for the specimen was some- 
 times covered by water. 
 
 I have observed little of this peculiar puddingstone in 
 Connecticut, though so abundant in the northern part of the 
 coal formation. It appears, however, in the south part of 
 Durham. 
 
 No, 60, Geest — covering a narrow valley. 
 
 No. 61. A narrow stratum of gneiss. 
 
 No. 62. Granite — This does not appear in abundance oh 
 the bank of the river. The best spot for examining it is 
 half a mile south, where it forms a hill 100 or iOO feet high. 
 
 From the preceding description of this profile, it appears, 
 that after crossing the first ridge of greenstone there is a 
 gradual decrease of the dip from 45° to 15°, and after pass- 
 ing this point, which is not exactly central, but nearer the 
 granite than the greenstone, we find the dip in a contrary di- 
 rection, and almost 90°. Precisely such would be the ef- 
 fect, the Huttonian would say, if we suppose the granife and 
 the greenstone to have been forced up tnrough the strata by 
 a subterranean fire, after these strata were consolidated. 
 And we might expect, also, that this convulsion would pro- 
 duce that wheeling of the strata observed in the central parts. 
 There is something peculiarly striking in this explanation, 
 and an inquiry arises, whether any corresponding facts oc- 
 cur in any other part of the coal formation. At mount To- 
 by, a few miles south of Gill and the highest point of the 
 coal formation, the strata dip to the east at an angle usually 
 less than 10°. And here the greenstone ridge on the west 
 is small, but the granite on the east, at no great distance, is 
 abundant. On the south east side of Mount Holyoke in 
 Belchertown and Granby, the strata dip to the south east, 
 near the mountain, at an angle not less than 45°, and the 
 greenstone ridge here is large. But the rocks that lie on 
 the back of Mount Tom, the highest point of greenstone 
 along the Connecticut, have a dip not generally larger than 
 20°. And the same remark will apply to many greenstone 
 ridges^ the accompanying coal formation in Connecticut.
 
 Geology, ^c. of the Connecticut. 71 
 
 The highest point of the coal formation is Mount Toby 
 in Sunderland, which rises between eight and nine hundred 
 feet above the Connecticut. Beginning at Whitmore's fer- 
 ry, the locality of the ichthyolites, to be hereafter described, 
 and passing up the mountain obliquely to the south-east, we 
 find alternations of most of the rocks described in the above 
 profile. The different varieties of conglomerate are most 
 abundant, and cannot, except that variety which is reddish, 
 be easily confounded with the conglomerate accompanying 
 the old red sandstone. They differ from this latter rock, 
 1. By being of a light or dark grey color, sometimes a 
 little red. 2. In the greater abundance of imbedded no- 
 dules, and less quantity of cement. 3. In the different na- 
 ture of these nodules, those in the old red sandstone con- 
 glomerate being chiefly quartz, felspar and granite, and 
 those in the coal formation pudding-stone, being chiefly 
 mica slate, argillite, chlorite slate, talcose slate, and quartz 
 with felspar and granite rarely. 4. The coal formation 
 pudding stone often contains thin incrustations of carbo- 
 nate of lime in the seams and crevices. The red sandstone 
 is w^anting in this. 
 
 As a general fact, I feel prepared to state that the rocks 
 of the coal formation lie above the old red sandstone. In 
 most cases these rocks are separated by greenstone, so that 
 their exact situation cannot be easily ascertained. Along the 
 western face of the greenstone ridge, extending from Mer- 
 iden into Massachusetts, the rocks of the coal formation are 
 often seen cropping out below the greenstone ; and the old 
 red sandstone occurs at a still lower level. This may be 
 seen in the space of a few rods in descending the hill nor- 
 therly, from Newgate prison ; and although the actual junc- 
 tion of the rocks is not here observable, yet they appear 
 only at short distances from one another. The fact, that 
 the coal formation alternates with greenstone, and that this 
 latter rock aiw^ays lies above the old red sandstone, is a 
 strong presumptive argument that all the coal formation 
 lies above the old red sandstone, and conclusive evidence that 
 a part of these rocks lie above it. The situation of the rocks 
 about Middletown, Chatham, &c. which might be urged 
 as an objection to this fact, has been already considered, 
 and I leave it for further examination.
 
 72 ■ Geology, ^c. of the Connecticut. 
 
 There are many instances, also, in which the rocks of the 
 coal formation pass into the old red sandstone. Let a per- 
 son go to the mouth of Fall river in Gill, where, as already 
 described, he will find the red argillaceous sandstone slate 
 of the coal formation cropping out below the greenstone. 
 Let him ascend Fall river, and he will find this slate be- 
 coming coarser, the layers thicker and the aspect changing, 
 until, within a mile and a half, it becomes decided old red 
 sandstone or conglomerate; the dip, also, diminishing, Or 
 let him follow the road that leads from the mouth of the 
 river to Greenfield, and as he ascends the hill, he will ob- 
 serve a gradation from the slate above named into decided 
 fine grained red sandstone. Much of the rock occurring 
 along the east side of Connecticut river in Somers, Elling- 
 ton, Chatham, in Middletown and Durham, appears to be 
 intermediate between old red sandstone and this slate of the 
 coal formation. Even in Somers and Ellington, where a 
 strip is marked as coal formation, I found little else but this 
 intermediate rock. But as coal has been found there, (Am. 
 Journal of Science, vol. 3, p. 248,) a strip has been colored 
 brown, rather to mark out the locality than the extent, of 
 the coal formation. It is not improbable that some more 
 experienced geologist than myself, may hereafter include 
 the rock I have marked old red sandstone on the east side 
 of Connecticut river as one of the members of the coal for- 
 mation — but I could not do it without doing violence to my 
 own convictions. 
 
 It may be of importance in a geological view to mention 
 the veins of copper ore so frequently found along the Con- 
 necticut greenstone ranges. All these veins which I have 
 seen, or of which an account has been published, are found 
 on tlie margin of the greenstone and coal formation; and 
 the veins always pass, either laterally or perpendicularlyy 
 from one rock into the other. They are quite numerous, 
 and we have already remarked that copper ore and iron 
 pyrites are not unfrequenlly disseminated in the slates. 
 
 To avoid mistake: I will just mention different spots on 
 the map that are colored as the coal formation. 1. A large 
 extent in Gill, Montague and Sunderland; 2. In Granby, 
 Mass. and Ludlow; 3 A small patch in Somers and El- 
 lington; 4. An extensive range extending from West- 
 Springfield to Berlin; 5. In Hartford, Westhersfield, Mid-
 
 Geology^ SfC. of the Connecticut. 73 
 
 dletown and Durham ; 6. A small patch in East-Haven j 
 7. A narrow range in Southington ; 8. The same in West- 
 field and South-Hampton. The latter, in the noriliern 
 part, is penetrated by the drift to the South-Hampton lead- 
 mine; but scarcely appears at the surface. In Westfield, 
 however, it is wider. 
 
 It would seem from the preceding description that all the 
 rocks essential to Werner's Independent Coal Formation 
 are to be found along the Connecticut, viz. a friable mica- 
 ceous sandstone, shale and pudding-stone, (Cleaveland, 
 vol. 2, p. 508,) and also the greenstone and amygdaloid 
 Professor Jameson has added. Still, however, there are 
 some other circumstances which may leave the geologist in 
 doubt whether the real independent coal formation occurs 
 along this river. 
 
 Some ma)' suppose the rocks above described to be grey 
 wacke and grey wacke slate ; and if the definition of grey 
 wacke be so broad as to include those pudding-stones whose 
 cement is merely a comminuted portion of the imbedded frag- 
 ments, it will indeed include not only the pudding-stone of 
 the coal formation above described, but, for aught 1 can see, 
 even the old red sandstone; and, indeed, what fragmented 
 rock will it not include.''* And besides, many of the argilla- 
 ceous sandstone slates described above, cannot, without diffi- 
 culty be distinguished from certain varieties ofgrey wacke slate 
 in hand specimens. But the rock usually called grey wacke 
 in Europe has never yet, I believe, been found lying above 
 the old red sandstone, as does the coal formation along this 
 river. It is usually traversed, say? Jameson, by quartz in 
 the form of veins, which is rarely, if ever, the case in our 
 rock. It has never been found alternating with beds of any 
 sort of coal, except the coal blende; but our rock con- 
 tains many beds and veins of that which is highly bitumin- 
 ous. Again, the icthyolites and other organic relics that 
 are found at Sunderland have almost all the rocks of the 
 ©oal formation lying above them, as may be seen by the 
 sketch of Mount Toby, that will be given when we come 
 
 *Some judicious remarks on this subject are contained in the North- 
 Aaierican Review, No. 29, p. 235. There we find the following sentenee 
 f oncerning the Roxbury and Dorchester plumb-puddino;-stonc, which some- 
 what resembles a certain variety described above. "This rock forms one 
 vast bed, which we have examined in various parts and feel no hesitation in 
 saying that it is not the grey wacke of European geologists." 
 
 10
 
 74 Geology, ^c. of the Connecticut. 
 
 to describe these remains. But in other countries "these 
 fossil remains of fishes are found only in strata of very re- 
 cent origin.'' (Rees. Cyc. Art. Icthyolltes.) 
 
 The great dip of many of these rocks may be thought to 
 afford evidence of their being older than the old red sand- 
 stone, or the independent coal formation. But to show 
 that the dip of rocks is a very equivocal criterion of their 
 age, I need only to refer to the recent work of Greenough 
 on the first principles of geology. And besides, it is no un- 
 common thing in real coal fields for rocks to be highly in- 
 clined. "This inclination or dip of the (coal) strata is found 
 every where ; in some places it varies very little from the 
 level; in others considerably, even so much as to be nearly 
 in a perpendicular direction;'' (Rees Cyclopedia, Art. 
 Coal,) and still farther, as already hinted, there is rea- 
 son to believe that Mount Toby, the strata of which 
 are almost horizontal, exhibits the original dip of these 
 rocks, and that those cases in which they are more 
 highly inclined are the result of some Plutonian convul- 
 sion. Such irregularity in the dip of coal fields is no 
 uncommon occurrence. "In some coal fields," says Mr. 
 Williams, (Nat. Hist. Min. Kingd. vol. 1, p. 93,) "the stra- 
 ta acquire this horizontal and waving position, and afterward, 
 towards the south-west or toward the north-east, the decliv- 
 ity becomes again so steep as to form an angle of 45°, and 
 in some particular instances to approach still nearer to the 
 vertical position." Upon the whole, I think there are insu- 
 perable objections against referring the rocks of our coal for- 
 mation to grey wacke and grey wacke slate. 
 
 Another opinion already advanced on the subject is more 
 probable. It is that of Mr. Brongniart, who gave it after 
 having seen only the rocks containing the Westfield fish 
 impressions. "This formation," says he, "appears to me 
 to have the strongest resemblance to that of the bituminous 
 marl slates of the copper-mines in the country of Mansfield 
 and Hesse." (Journal of Science, vol, 3, p. 220.) The 
 arguments in favor of such an opinion are, 1. The great sim- 
 ilarity in the appearance of the German and American rocks 
 on which the fish are found — one species, at least, being 
 the same in both, 2. Tlie occurrences of copper ores, and 
 similar o:;es too, along with native copper in both rocks. 
 3. The fact that both these varieties of rocks lie immedi- 
 ately above the old red sandstone. Perhaps there are oth-
 
 Geology, S^c. of the Connecticut. 75 
 
 or points of resemblance, but I have not been able to find 
 any minute account of the bituminous marlite formation.* 
 
 On the other hand it may be said that no real bituminous 
 marlite occurs along the Connecticut — provided the grand 
 distinction between this rock and bituminous shale consists, 
 as Professor Cleaveland says, (Mineral, vol. 1, p. 191,) in 
 its effervescence with acids ; for our rock, certainly that at 
 Sunderland, does not effervesce with acid, unless it contains, 
 as it sometimes does, a slight incrustation of carbonate of 
 lime. Mr. B. does not consider the occurrence of thin 
 beds or veins of coal as opposed to his opinion; but the 
 strata penetrated at Riegelsdorf in Hesse, in order to reach 
 the fish impressions, are totally different from those occur- 
 ring along the Connecticut. They are as follows: " No. 1, 
 Ferruginous clayey mould, from one to two fathoms. No. 
 2. Greyish white limestone, from six to eight fathoms. ' 
 No. 3. Blue clay, with imbedded fragments of selenite 
 crystals, from eight to ten fathoms. No. 4. Bluish lime- 
 stone, called Rauchivacke, from eight to nine fathoms. No. 
 5. Grey compact gypsum, traversed by ferruginous loam, 
 from seven to eight fathoms. No. 6. Black and grey stink- 
 stone, from one to one and an half fathoms. No. 7. Sand, 
 sometimes loose, sometimes cemented, from one to one and 
 an half fathoms. No. 8. A kind of limestone, called Zech- 
 stein, of a greyish brown color, and soft above towards the 
 sand, but blacker and more compact below; from three and 
 a quarter to three and an half fathoms. No. 9. A black 
 slaty stratum, containing pyrites and forming the roof of the 
 bituminous marl slate, from eighteen to twenty inches. No. 
 10. Black cupriferous bituminous marl slate, from three to 
 eight inches : this is the principal depository of the icthyo- 
 
 *Extract of a letter from Dr. J. W. Webster : — 
 "The bituminous marl slate has been one of the most troublesome rocks 
 for years : some have placed it here and some there. From its effervescence 
 with acids we should perhaps more properly put it among the limestones. 
 Again, from the richness of some specimens of it in copper, they would be 
 classed as copper ores — indeed, we know that it is worked for copper. It 
 occurs in the secondary limestone. Its external characters are very little 
 different from those of bituminous shale of the coal formation ; but from all I 
 have learned of it, I am pretty well satisfied that it is distinct from and above 
 the rocks of the coal formation. You will note one striking difference be- 
 tween the two — vegetable impressions are abundant in bituminous shale of 
 the coal field ; but rare in the B. M. slate — it is more abundant in fresh 
 water remains."
 
 76 Geology, (^c. of the Connecticut. 
 
 lites. No. 11. Gneiss like greyish white rock, consisting 
 ol' small rounded quartz pebbles, and sometimes of copper 
 and mica, cemented by indurated clay. No. 12. Old 
 red sandstone, or the dead rock, being the fundamental 
 rock of these floetz strata." (Rees Cyc. Art. Icthyoiites.) 
 
 Under these circumstances I have thought it safe to de- 
 nominate the peculiar rocks under consideration along the 
 Connecticut, the coal formation. A more complete set of 
 them has been forwarded to Mr. Brongniart, and we wait 
 anxiously for his final opinion. The suspicious circumstan^ 
 GPS attending them and the occurrence of the coal hitherto 
 discovered in thin beds and veins only, render it very doubtful 
 whether extensive beds of this valuable mineral will ever be 
 found in them. They have been unsuccessfully explored 
 at South-Hadley, Southington and Westfield, Ct. But I 
 would not wish to discourage further search. The decision 
 of the question above discussed, concerning the precise 
 lank they ought to hold in the rock formations of the globe, 
 is one of considerable importance, since it will depend on 
 that decision whether coal or copper or gypsum may be 
 sought after with the greatest prospect of success. They 
 liave long been to me a fruitful source of perplexity, and 
 again and again have I returned from traversing them in 
 utter despair of ever determining their real geological rela- 
 tions. To denominate them the coal formation relieves, 
 ibr a time, most of these difficulties : but that name will 
 cheerfully be resigned whenever a more correct one shall 
 1)6 proposed. 
 
 Organic Remains in the Coal Formation, 
 
 1. Icthyoiites. 
 
 These occur at Westfield, Ct. and at Sunderland, Mass. ; 
 and it is said also at some other places, as at West-Spring- 
 field ; but I have never seen any, except from these two 
 localities. At Westfield they were found in exploring for 
 coal, \y'it^ upon bituminous shale. Two species at least 
 were recognized, one of which Mr. Brongniart calls the Pa- 
 Icethrissum freislebenense of Blainvilie. These impressions 
 have been so repeatedly and accurately described by Prof. 
 Silliman in Cleaveland's Mineralogy and the American 
 Jour, of Science, that it is unnecessary to be more particular.
 
 Geology., <^c. of the Connecticut. 77 
 
 At Sunderland these impressions occur in bituminous 
 shale, which often contains a little mica, and generally a 
 quantity of iron pyrites, disseminated through the rock. 
 They occur at Witmore's ferry in the north part of Sunder- 
 land, in the bank of the river. They are found most abun- 
 dant at the lowest water mark, at which time two men, in 
 less than half a day. dug out for me nearly fifty specimens. 
 Sometimes a layer of semi-crystalline dark colored carbo- 
 nate of lime, less than one twentieth of an inch thick, lies 
 between the layers of slate. The substance of the fish is 
 usually converted iiUo coal, the thickness of which is rarely 
 more than one tenth of an inch in any part, and the color is 
 black. In some instances, however, the carbonate of lime 
 above mentioned covers the fish, and has taken the place of 
 the matter of the fins and scales and their original light 
 grey color isp;eserved so perfectly as to resemble a fish 
 just taken out of the water. Some of the specimens 
 appear contorted; in others the form of the fish is whol- 
 ly lost, the fins and scales and bones, being scattered 
 about promiscuously, as if the fish had perished in violent 
 struggles or the rock had been disturbed after its imprison- 
 ment. Yet, in the same specimen that contains one thus 
 mutilated, another will appear not more than a foot distant 
 which is whole. 1 have found four or five specimens in 
 which the fishes (both of them distinct,) lie across each oth- 
 er; sometimes a very thin layer of shale, and sometimes 
 none, separating them. I have another specimen, three feet 
 longand fifteen inches wide, containing seven distinct impres- 
 sions. The shale in which these ichthyolites occur,when rub- 
 bed or held in a flame, exhales a strong bituminous odour.*' 
 
 Among the impressions hitherto obtained, I can easily 
 discover three distinct species that have scales * Two of 
 these are represented on the accompanying plate ; but the 
 third was so much mutilated, that 1 did not attempt to de- 
 lineate it. For at the best it is no easy matter to represent 
 them so exactly as to be of use. They are usually a little in- 
 distinct on their border,and not unfrequently injured by pyrites. 
 
 Fig. 1. represents a species that is rare. 
 
 Fig. 2. shows the most common species. There can be 
 no doubt that this differs generically from the last. 
 
 *Precisely such a smell is exhaled from the bituminous limestone in 
 Southington. 
 
 *Sce the en<3.
 
 "^S Geology, c^c. of the Connecticut. 
 
 Fig. 3. is probably the same as Fig. 2. ; but perhaps not. 
 The outline is given because the fins were more distinct 
 than in the specimen from which Fig. 2. was copied. 
 
 These are all of the natural size. Concerning their names, 
 feeling altogether incompetent, I do not even attempt to de- 
 cide. I have not had an apportunity to compare them close- 
 ly with the Westfield icthyolites, and do not know whether 
 they coincide. 
 
 Another petrifaction occurs with these fishes, which re- 
 sembles the common silver eel, (Muraena anguilla.) or some 
 other species of the eel tribe. The width varies from half 
 an inch to a whole one, and the length from one to two feet. 
 The substance of the eel (if indeed it be one,) is not con- 
 verted into coal, but there is a substitution of the shale of a 
 finer grain, except the head, which is coal. No fins appear, 
 except, perhaps, in one instance, a pectoral one. Some- 
 times, along the centre of the impression, there is a small 
 relief, answering to the place of vertebrae. The course of 
 the impressions is usually serpentine. 
 
 The geological situation of these icthyolites is interesting. 
 The shale containing them passes under Mount Toby, there 
 being a gradual ascent from this spot to the top of the 
 mountain, two miles distant : so that they lie beneath rocks 
 of the coal formation at the depth of nearly nine hundred 
 feet, most of the varieties described on the profile annex- 
 ed to the map here alternating with one another. The fol- 
 lowing sketch exhibits a section of the shale of Mount Toby, 
 so far as the geest would admit of examination, on a line 
 passing from the locality of the icthyolites to the highest 
 point of the mountain. I do not suppose it perfectly accu- 
 rate , but it is probably sufficiently so to answer the intend- 
 ed purpose, viz. to exhibit the situation of the ichthyolites. 
 The numbers in a parenthesis refer to those on the profile 
 that are synonymous. The dip of these strata rarely ex- 
 ceeds ten degrees, and is usually less. 
 
 No. 1. (No. 59.) Very Coarse dark grey pudding-stone^ 
 for an account of it see the reference to the profile, on 
 plate No. 8. at the end. 
 
 No. 2. Bituminous Shale. This contains icthyolites — 
 strata nearly horizontal — dip never exceeding five degrees. 
 Thickness of the stratum, about ten feet. 
 
 No. 3. Same as No. I . except sometimes alternating with
 
 Geology, S^c. of the Connecticut, 1% 
 
 a pudding-«tone, less coarse and more distinctly stratified. 
 Thickness, between tv^^o and three hundred feet. 
 
 No. 4. (No. 9.) Red fissile argillaceous sandstone slate, 
 ten feet in perpendicular thickness. 
 
 No. 5. Same as No. 1. Thickness ten feet — dip six de- 
 grees. 
 
 No. 6. Same as No. 4. Thickness four feet. 
 
 No. 7. Same as No. 1. except not so coarse, and more 
 distinctly stratified, agreeing nearer with No. 43 of the pro- 
 file. Thickness fifteen feet. 
 
 No. 8. Same as No. 4. two feet thick. Where this rock 
 alternates with the pudding-stone the change is very strik- 
 ing. 
 
 No. 9. Same as No. 7. Thickness fifteen feet. 
 
 No. iO. Same as No. 4. five feet thick. 
 
 No. 11. Same as No. 7. twenty feet thick. 
 
 No. 12. Same as No. 4. graduating into the conglomer* 
 ate — ten feet thick. 
 
 No. 13. Like No. 1. sixty feet thick. 
 
 No. 14. Grei/ argillaceous sandstone slate, sometimes 
 micaceous. Somewhat like No. 23. of the profile, but 
 coarser — liable to decomposition and containing many wa- 
 ter-worn pebbles. Thickness ten feet. This carries us to 
 the Sunderland cave. 
 
 No. 15. Same as No. 4. fifteen feet thick. 
 
 No. 16. Same as No. 1. about one hundred feet thick. 
 
 No. 17. Same as No. 4. except that it is coarser and the 
 layers thicker — about ten feet thick. 
 
 No. 18. A pudding-stone not differing essentially from 
 No. 1. but frequently of a reddish cast and more distinctly 
 stratified. This continues with little interruption to the top 
 of the mountain ; though the soil hides it in most parts, and 
 there may be other alternations which I did not observe. 
 
 2. ^ Clam Shell? 
 
 I found a specimen at the cave in Sunderland, imbedded 
 in an argillaceous slate, which resembles the common river 
 clam. There was a perfect substitution of siliceous matter. 
 A single specimen only was found, which was forwarded to 
 Mr. Brongniartj and he will be able doubtless to decide 
 "whether it is a petrifaction or a peculiar water- worn pebble.
 
 Sj9 Geology, S^rc. of the Connecticut. 
 
 3. Vegetable Remains. ' 
 
 These appear to be either the branches or roots of trees, 
 or the relics of cuhniferous plants, and therefore may be cal- 
 led lignites and rhizolites. They are usually converted in- 
 to a thin vein of coal, similar to the fish. They are com- 
 monly broken into pieces from an inch to two feet long, in 
 the manner represented in Fig. 4. Their width varies from 
 a mere line to two inches. They are not jointed — found in 
 abundance at the falls in Gill ; also with the icthyolites at 
 Sunderland. The rock in which they occur at both places 
 is hardly bituminous shale ; but a greyish micaceous sand- 
 stone. The longest specimen of rhizohte 1 have seen oc- 
 curs on the road side, one half mile south of Newgate pris- 
 on; being not less than seven or eight feet in length. 
 
 4. Unkn07on Relic. 
 
 This is represented as well as it could be in Fig. 5. It 
 is difficult to give a perfect idea of the thing, because there 
 is a relief or swelling along the middle. It sometimes re- 
 sembles the anient of the chesnut, (Caslanea americana 
 Mx.) but still more the vertebrae of a fish. But in no ich- 
 thyolite I ever found, did I see any remains of the vertebrae, 
 and it is not probable, therefore, that this belonged to a fish. 
 It is rare — found with the icthyolites at Sunderland. 
 
 15. Alluvion. 
 
 Colored Gamboge Yellow, 
 
 By this term I understand those accumulations of gravel, 
 clay, sand, mud and salt, which are post-diluvian, or have 
 probably been deposited since the Noachic delude by causes 
 at present acting on the globe. Some varieties may be 
 seen along the Connecticut which we shall mention in the 
 probable order in which they were deposited. 
 
 1. The alluvion on the sea-coast. This is probably the 
 oldest; because the sea would begin its depositions imme- 
 diately after the deluge, if the situation of any particular 
 place were favorable — even before it had subsided suffi-
 
 Geology, ^c. of the Connecticut. 81 
 
 ciently for rivers to have found their channels. On the 
 map it embraces the alluvial plain around New-Haven and 
 the salt marshes extending some distance on both sides of 
 the city . The plain of New-Haven is made up of coarse 
 sand vv 'th some gravel and an intermixture of broken shells 
 and sea weed. The marshes consist of sand, mud and 
 salt. 
 
 The region about New-Haven, embraced by this alluvion, 
 is interesting to the botanist, as he here finds many plants 
 not growing in the interior. Among these, we may men- 
 tion Salsola kali, Salicornia herbacea, Triglochin mariti- 
 mum, Statice limonium, Iva frutescens of Lki. and Ammi 
 capillaccum and Conyza camphorata of Muhl. Limnetis 
 polystachia and juncea of Ph. L. glabra, Muhl. Holciis 
 odoratus, Mx. and Limosella suhulata, Ives. Here also, 
 occur the other new species of Prof. Ives, GnaphaUum de- 
 currens and Asclepias lanceolata, along with Plantago 
 maritima, lanceolata^ and Virginica of Lin. Eriocaulon 
 pellucidum, Mx. Cassia chamaecrista and Uniola spicata 
 of Lin. &.C. &LC. On the beach we find Fucus nodosus 
 and vesiculosus of Lin.* and adhering to the latter, 
 Mytilus striatuhis ? (Donov. in Rees.) Here also occur 
 Venus mercenaria, (common clam) Ostrea edulis ? (oyster) 
 and one or two species oi Area and Anomia, with others I 
 do not know. 
 
 2. Gravel. This usually lies beneath all other alluvial 
 deposits along the Connecticut : though it sometimes al- 
 ternates with beds of sand. It is arranged in somewhat 
 regular strata. The pebbles rarely exceed two or three 
 inches in diameter. 
 
 3. Clay. This is a coarse kind, such as is used for mak- 
 ing brick; and generally lies above the gravel and beneatli 
 the sand and mud, or loam. It probably underlies those 
 extensive sandy plains that occur in Suffield and Windsor, 
 on the West, and in Springfield, Longmeadow, Enfield, 
 East Windsor, and East Hartford, on the east of the Con- 
 necticut. In some places the clay appears at the surface, 
 as in Hartford, Windsor, Deerfield, Sic. 
 
 * On Long-Island, fifty miles east of New-Haven harbor, I found Sphae- 
 roroccns covfervoidcs, Agardh. 
 
 11
 
 82 Geology., <^c. of the Connecticut. 
 
 4. Sand. This commonly lies the highest of the alluvi- 
 on, except in some low meadows that are yearly receiving 
 a deposite of a loamy sediment. The region in which 
 sand occurs most abundantly, has just been mentioned. It 
 is sometimes seen in alternating beds with gravel, clay and 
 loam. 
 
 b. Loam and mud. This is the most recent of our allu- 
 vion, and depositions of it are frequently made. The Con- 
 necticut indeed, seems, with some exceptions, to have 
 nearly reached its maximum of depositions, rarely flowing 
 over more than a small part of the alluvion along its banks. 
 But its tributaries, such as the Farmington, Westfield, Deer- 
 field, and Chickapee, still continue annually, and often 
 semi-annually, to flood the adjacent meadows, and to leave 
 there an additional soil, from half an inch to six inches 
 deep, and though the agriculturalist has sometimes to la- 
 ment the destruction of his crops by these inundations, yet 
 without them his fields would soon become comparatively 
 unproductive. 
 
 The depth of the alluvion along the Connecticut has 
 never been accurately measured ; but I should judge it 
 sometimes to be as great as one hundred and fifty feet;: 
 but in general it is much less. It is not unfrequent to find 
 ten or fifteen feet below the surface of the most recent of 
 this alluvion, logs, stumps of trees, leaves, butternuts, wal- 
 nuts, &c. in a partially decaying state, and sometimes we 
 meet with skeletons of the aborigines of the country. But 
 no aurock, mastodon, or megatherium, has yet been dis- 
 covered to give an interest to this alluvial formation. 
 
 I have found a difliculty in some instances in drawing the 
 line between genuine post-deluvian depositions and geest. 
 In some cases there appears to be a mixture. In other 
 cases the rocks are entirely hid by the soil, and yet the 
 predominant characteristic of the soil is derived from the 
 rock underneath it, although there is a mixture of alluvion. 
 The old red sandstone for instance, and the red slate of the 
 coal formation, are very liable to decomposition, and thus 
 a reddish soil is produced, so manifestly composed of the 
 ruins of the rock, that one is able often to determine from 
 the appearance of the soil at the distance of two or three 
 miles the particular rock that lies beneath it. I have not.
 
 \ 
 
 Geology., ^c. of the Connecticut. 83 
 
 however, intended to put down the alluvion in all such cases, 
 but have colored the spot according to the subjacent rock. 
 And on this ground I am sensible that there are a number 
 of small parts of the alluvion that ought, in strictness, to 
 have been colored as old red sandstone ; as in East-Hamp- 
 ton and Deerfield ; but being so small they were neglec 
 ted. 
 
 16. Geest. Jameion. 
 
 Deluvian Detritus. Buckland. 
 
 •'By geest," says Jameson, "is understood the alluvial 
 matter which is spread over the surface both of the hilly 
 and low country and appears to have been formed the last 
 ti me th e waters of the ocean stood over the surface of the 
 cjMHI And it is probable that Professor Buckland refers 
 to the same deposition by the above synonym. By deluvi- 
 an detritus, he means "fragments of neighboring and dis- 
 tant rocks, and with bones not mineralized — generally in 
 valleys." Whatever objections may lie against these defi- 
 nitions, every geologist knows that much deposition exists 
 on the globe which no one refers to what is commonly un- 
 derstood by alluvion, and which could result from no pro- 
 cesses nature is now carrying on. This is scattered over 
 the most mountainous tracts, and in all cases of consider- 
 able extent, occupies at least three quarters of the surface. 
 It is usually denominated soil, comprehending, however, 
 the bowlder stones and organic remains that soil contains. 
 As a general fact, this geest, in primitive regions, consists 
 of comminuted particles and rolled stones of primitive 
 rocks. In secondary tracts it consists of secondary detritus, 
 though more frequently mixed with portions of rocks of a 
 primitive character. 
 
 Along the Connecticut in the primitive region, large 
 bowlders in great numbers are not commonly found remov- 
 ed many miles from the spot where they originated. Strag- 
 glers of this description may indeed be found almost every 
 where ; and among all the rocks none seems to be more 
 scattered than granite : though perhaps the numerous beds 
 and veins of this rock found almost every whrre may ac-
 
 S4 Geology, ^c of the Connecticut. 
 
 count for this. But in general along this river, the char- 
 acter of the rolled masses corresponds to the rock in place 
 underneath them ; — that is the greatest number of the 
 loose stones are of the same description as the rock that 
 underlies them. But to this there are many exceptions — a 
 most remarkable one occurs a few miles west of New- 
 Haven in Woodbridge and Milford. The surface is cover- 
 ed with rolled masses, sometimes quite large, of primitive 
 and secondary greenstone, mica slate, gneiss, granite, and 
 almost every other rock, except that which is in place 
 viz. chlorite slate, or argillite. In many places on the map 
 which are highly mountainous, the geest is so abundant 
 as to occupy most of the surface ; — the subjacent rock 
 rarely appearing ; — as in the east part of Plainfield and in 
 Shutesbury. The diameter of the loose fragments varies 
 from an inch to twenty, or even thirty feet, and they are 
 usually rounded, indicating attrition. Some of the|j|||^est 
 of these bowlders are found insulated on the pinnacles of 
 our mountains. 
 
 There is a particular kind of geest, which I have al- 
 ready mentioned, occurring along the Connecticut, that 
 does not seem to be comprehended in Professor Jameson's 
 definitions. It is that kind of soil that results from the 
 slow disintegration and decomposition of certain rocks, 
 with a mixture of decaying vegetables. This, as already 
 observed, is not uncommon above the old red sandstone 
 and the red siliceous sandstone slate of the coal forma- 
 tion, ^nd the epithet delnvian seems to exclude this kind 
 of soil from Prof. Buckland's deluvian detritus; and so the 
 epithet fiuviatile excludes it from the jluviatile detritus of 
 the s?.n)e author. (Rees' Cyc. Art. Geology, Addenda.) 
 
 Hayden^'s Hypothesis of a primeval northeasterly current of 
 
 water. 
 
 1 allude to Haydcn's Geological Essays, in which he ex- 
 presses ihe opinion that the alluvion of our middle and 
 southern states was formed by a current or currents that 
 formerly flowed across this continent from the northeast to 
 the southwest; and I am inclined to believe, (without in- 
 tending, however, to adopt altogether his theory on the
 
 Geology^ <$'C. of the Connecticut. 85 
 
 subject,) that a careful examination of the bowlder stones 
 along the Connecticut would favor the supposition. Mas- 
 ses of greenstone are found at a greater distance, and in 
 much greater quantities on the western side of the ridges 
 than on the eastern. As we ascend the primitive region 
 on the west side of ihe river, secondary rolled stones are 
 seen for one or two miles ; but on the eastern side, if I 
 mistake not, nothing of this kind appears; and 1 should 
 suppose the bowlders of Woodbridge and Milford, being 
 evidently brought from the country to the north, would tes- 
 tify in favor of such an hypothesis. 
 
 Suggestion concerning rolled Stones. 
 
 Is it not a fact that rolled masses are more abundant and 
 more perfectly rounded along the limits between the primi- 
 tive, and transition, or secondary ? This question has often 
 occurred to me when travelling in the south eastern pai-t of 
 Massachusetts, when going over the country along the 
 Connecticut in Bernardston and its vicinity, when descend- 
 ing the Hoosack and Green Mountains on the west, and 
 when passing over the country west of New-Haven. It 
 such be the fact it may, when it occurs in the geologist's 
 tours, be a warning to him to expect a change iu the rocks 
 in place. 
 
 Fact relating to the detachment of large bozoldcf stones from 
 their bed. 
 
 Deerfield river in the greater part of its course is a 
 mountain torrent, very rapid and powerful. It has worn 
 a passage often four hundred feet deep, the banks being al- 
 most perpendicular. Its winter floods are most powerful 
 in effecting this work. The ice freezes three or four feet 
 thick, and when a sudden rain melts the snows on its banks, 
 it rises rapidly and lifts up and urges forward with tumultu- 
 ous fury, this immense body of ice. As the banks among 
 the mountains are steep and rocky, they prevent the ac- 
 cumulation of water and ice from spreading to the right or 
 left, and it is raised proportionally higher ; and thus an im- 
 mense force is exerted upon obstacles in the bottom of the
 
 86 Geologi/, ^-c. 'of the Connecticut. 
 
 stream, which, in winter floods, is filled with huge masses 
 of ice to the very bottom. 
 
 In the west part of Shelburne this river descends a cata- 
 ract thirty or forty feet high. The rock in the bottom of 
 the river is an aggregate of quartz and mica with horn- 
 blende intermixed, and below the falls it is unstratified, al- 
 most without seams and very hard. Yet here we might 
 expect the force of the torrent would be most powerful ; 
 and accordingly we find masses of this rock from one to. 
 ten feet in diameter, raised from their bed, and some of 
 them removed down the stream one or two miles, some only 
 a few rods, and I saw one or two of the largest but just be- 
 ginning to be raised from their bed. Previous to viewing 
 this spot, I had no just ideas of the enormous force exerted 
 by a mountain torrent.
 
 GEOLOGY, MINERALOGY, TOPOGRAPHY, &c. 
 
 OF THE CONNECTICUT. 
 
 PART II, 
 
 Simple Minerals. 
 
 Metallick Veins and Beds. 
 
 Before giving a list of the simple minerals found along 
 the Connecticut, it may perhaps be acceptable to the geolo- 
 gist, to present a short account of those veins and beds of 
 ore, that occur in the district, which either have been, or 
 may be wrought as mines. 
 
 1 . Southampton Lead Mine* 
 
 This is a vein containing sulphuret, carbonate, sulphate^ 
 molybdate, muriate and phosphate of lead, with blende, py» 
 ritous copper, &ic. The gangue is quartz, with sulphate 
 
 * For a description of thig mine, by Professor Silliman, who examined it 
 in May 1810, see Bnicc's Journal, Vol 1, p. 63. 
 
 13
 
 88 Geology, <^-c. of the ConnecticuU 
 
 of barytes and fliior spar intermixed. The vein declines ten 
 or fifteen degrees from a perpendicular; is six or eight feet 
 in diameter, and traverses granite and other primitive rocks. 
 It has been observed at intervals from Montgomery to Hat- 
 field, a distance of twenty miles : but it is very doubtful, 
 whether it continues, uninterruptedly, the whole of that ex- 
 lent; indeed, from what I have observed of other lead veins 
 in the vicinity. I have sometimes been disposed to ques- 
 tion, w'hether the veins observed at many of these intervals, 
 may not be totally distinct from one another. In Southamp- 
 ton, ei-ht miles south west from Northampton, is the only spot 
 where this vein has been extensively wrought. In that 
 })!ace it has been explored thirty or forty rods in length, to 
 the depth of forty or fifty feet, and the galena, which is the 
 principal ore, has been found in masses from a quarter of an 
 inch, to a foot in diameter. At the depth above mentioned, 
 the water became so abundant, that it was thought advisable 
 to abandon a perpendicular exploration, and to descend to 
 the foot of a hill on the east, nearly eighty rods from the vein, 
 and attempt a horizontal drift, or adit, and ever since its 
 commencement, seven or eipht years ago. the working of 
 the vein has ceased. This drift is now carried into the hill, 
 on an exact level, nearly sixty rods, and the workmen told 
 me, that not less than 20,000 dollars had been expended 
 upon it. The rocks that have been penetrated, reckoning 
 from the mouth of the drift inwards, are geest, the red and 
 gray slates of the coal formation, ("granulated schistose ag- 
 gregate." Eaton. Journal of Sci. Vol.1, p- 136,) with thin beds 
 of coal, and mica slate, and granite alternating. Probably 
 the fundamental deposit of granite is now uncovered ; and 
 the principal vein of galena cannot be far distant. Several 
 small branch veins of crystallized quartz and galena have 
 been crossed ; and several specimens of these, collected by 
 Dr. Hunt, were very rich and beautiful ; the crystals of pure 
 galena sometimes exhibit, on their faces, insulated crystals 
 of honey coloured carbonate of lime. The principal vein 
 will be found not less, I should judge, than one hundred and 
 fifty feet below the surface : — and when that time comes, it 
 is confidently expected, not only that the proprietors will be 
 rewarded for the great expence they have incurred, but, al- 
 so, that many a rich specimen will be found to ornament the
 
 Geology, ^'c. of the Conneclicut. 89 
 
 mineral cabinets of oiu- country, and to vie in beauty with 
 the lead ores of Europe. 
 
 The mouth of this drift is four or five feet wide, and about 
 three feet above the surface of the water. The water is 
 deep enough, the whole length of it, to admit the passage of 
 a loaded boat. TJie person wishing to explore this internal 
 canal, must fire a gun at the entrance, or i^eat heavily with 
 a sledge on the timbers that support the soil; in ten or fif- 
 teen minutes he will perceive a gentle undulation of the wa- 
 ter, and soon after a boat advancing with lighted lamps and 
 a rower; having seated himself on the bottom of this boat, 
 and provided himself with an additional garment, he is pre- 
 pared for his subterranean expedition. As he enters the 
 passage, he will, for a moment, experience, or imagine he 
 experiences, a little difficulty of breathing. But he will 
 soon become reconciled to his condition ; and after passing 
 about one hundred feet in the excavation, for which distance 
 the soil is supported by timbers, he will find occasionall}' 
 more room, so that he can ^tand erect. If he looks back, 
 after having advanced several hundred feet, the light at the 
 entrance will appear diminished to the size of a candle; and 
 before he reaches the extremity, it becomes invisible. About 
 halfway from the entrance to the end of the drift, he will 
 pass a shaft ; down which a small brook is turned, for the 
 purpose of aiding the ventilator. When he reaches the 
 end of the drift, he finds himself to have penetrated nearly 
 sixty rods chiefly into solid rock; a voyage which although 
 inferior to that performed in the celebrated navigation mine, 
 in the Peak of Derbyshire, is still extremely interesting. 
 
 The miners do not quit the drift when they blast ; but re- 
 tire behind a breast work thrown up for the purpose. En- 
 teriiig immediately after an explosion, I did not perceive the 
 air to be in any degree more oppressive than when powder 
 is fired above ground. One man told me that he had been 
 an inmate of that dark recess, eight or ten years, without 
 suffering in his health, and when he returned alone into his 
 dreary prison after conducting me to the day ligiit, he struck 
 up a cheerful song, indicating buoyant spirits and a content- 
 ed mind. 
 
 Every mineralogist passing that way, will of course visit 
 this drift. Intelligent gentlemen without professional views,
 
 90 Geology, S/c. of the Connecticut. 
 
 and even ladies not iinfrequently enter this cavity, and find 
 themselves amply repaid for their trouble.* 
 
 2. Vein of Galena in Whately. 
 
 This occurs in the north west part of the town, and I for- 
 merly supposed it a roniinuation of the Southampton vein. 
 But the Southampton vein runs north east and south west, 
 and this in Whately almost exactly north and south. Be- 
 sides, the Southampton vein must turn almost at right angles 
 from Hatfield, in order to be found in the north west part of 
 Whately. 
 
 This vein m;!y be traced at intervals one hundred rods, 
 and extends into the edge of Conway. At the extremities 
 it traverses mica slate ; but in the middle, it cuts through an 
 extensive bed of granite. Its diameter is usually s-ix or sev- 
 en feet, and the gangue is wholly common and radiated 
 quartz. Galena, which is the only ore found in this vein, 
 is disseminated through this matrix in considerable abun- 
 dance. Very few efforts have been made to explore this 
 vein, though appearances at the surface are not unfavora- 
 ble ; and if a horizontal drift were necessary, a deep valley 
 within a few rods on the west, would afford a favourable op- 
 portunity for making it. As nearly as I could determine, this 
 vein is not far from perpendicular to the horizon. 
 
 3. Vein of Galena in Leverett. 
 
 In the.jsouth west part of the town — traversing granite — 
 only a foot wide — gangue, sulphate of barytes — deviation 
 north and south — galena the only ore. 
 
 4. Vein of Galena, Pyritous Copper and Blende, in Leverett. 
 
 About two miles north of the vein last mentioned; and it 
 may be a continuation of it. The gangue is quartz, united 
 with sulphate of barytes ; and the galena and pyritous cop- 
 per are disseminated through it in nearly equal quantities. 
 
 * I have often thought Professor Cleaveland must have selected the ap- 
 propriate motto prelixed to his Mineralogy, when entering this or some 
 similar drift. 
 
 • itumest in viscera terrae i-c.
 
 Geology, ^c. of the Connecticut, Q) 
 
 The blende is much les's abundant. The vein is several feet 
 wide, traverses mica slate and granite, and has been conside- 
 rably wrought. 
 
 5. Lead Mine at Middletown. 
 
 I am unacquanted with the geological situation of this 
 mine. 1 put ii down on the authority of Professor Silliman 
 in Cleaveland's Mineralogy. 
 
 6. Vein of Galena at Bethlehem. 
 
 I mention this on the same authority without any persoa- 
 al knowledge of it. It is, however, a little beyond the lim- 
 its of the map. 
 
 7. Vein of Galena and Pyritous Copper in Southington. 
 
 Same authority — gangue, sulphate of barytes and quartz, 
 I believe this vein occurs in the coal formation. 
 
 8. Mine of Galena, Blende and Pyrites in Berlin* 
 
 This occurs in greenstone, at its junction with the coal 
 formation. The gangue is sulphate of barytes. The galena 
 crystals are small ; those of the blende larger ; th > pyrites is 
 the least abundant. The vein is not now wrought. (Vide 
 Dr. PercivaPs Notice, Journal of Science, Vol. 5. p. 44.) 
 
 Copper Mines and Veins. 
 
 It has already been mentioned, in the geological part of 
 this sketch, that these ores (like the mine of galena Sic. last 
 mentioned,) exist along the junction of the greenstone with 
 the coal formation. The veins frequently pass into both 
 rocks, and are of various sizes and of frequent occurrence. 
 Indeed, they may be found probably every mile or two 
 along the line, where these rocks unite. A few of them, 
 that have obtained some notoriety will be mentioned.
 
 92 Geology^ S/c. of the Conneciicul. 
 
 9. Vein of Pyritous Copper and Green Carhonaic of Copper, 
 
 at Cheshire. 
 
 In greenstone and associated with sulphate of barytes, 
 quartz, carbonate of lime and sandstone. (Silliman in 
 Cleavelaud's Mineralog}-, Vol. 2, p. 569.) 
 
 10. Mine of the Red Oxide of Copper, Green Carbonate of 
 
 Copper, ^'C. Granhy. 
 
 This is better known by the name of Simsbury Mines al- 
 though it occurs within the boundaries of Granby. It was 
 formerly wrought, but being at length abandoned, its shafts 
 and galleries were converted into a state's prison. The 
 mineralogist who explores this spot, must here contemplate 
 the painful spectacle of almost every variety of guilt and crime. 
 Sixty or seventy whites, mulattoes and negroes, scarcely 
 distinguishable through filth, from one another, are here com- 
 pelled by the point of the bayonet to labour at the anvil; 
 while we read in their sullen and ghastly countenances, the 
 inward w-orkings of hearts rendered desperate by crime 
 and punishment. As we descend into the shaft we observe 
 the offensive recesses in the rocks, where these prisoners 
 were formerly confined during the night. But only a few 
 of the most refractory are now compelled to sleep in these 
 damp and dismal dungeons; the government of Connecti- 
 cut being satisfied that this kind of rigor served rather to 
 harden than to reform the criminal. About seventy feet be- 
 low the surface, the conductor pointed out to me a bolt 
 driven into a wet rock, where, recently, one of the prison- 
 ers had been fastened for a week or fortnight, as an extra 
 punishment for peculiar obstinacy; and where he lay, I saw 
 scattered, the leaves of a bible, which, in his desperation he 
 had torn in pieces: — thus spurning alike the laws of God 
 and man ! 
 
 If we judge from the present appearance of this excava- 
 tion the original vein of ore must have been extremely ir- 
 regidar, forming bellies and f7vilchrs. It passes through the 
 greenstone and enters the red and gray micaceous sand- 
 stone of the coal formation, which underlies the greenstone. 
 All the varieties of ore I saw at the place were the red ox-
 
 Geology, ^c. of the Connecticut. 93 
 
 ide disseminated in sandstone, and mixed with a small pro- 
 portion of green carbonate of copper. How productive tliis 
 mine has been, I do not know. 
 
 1 1 . Vtin of Green Carbonate of Copper and Pyritous Copper 
 in Greenfield Mass. 
 
 This is found on the west bank of Connecticut River, 
 one hundred rods below the mouth of Fall river, and about 
 the same distance in a direct line from Turner's Falls. It 
 occurs at the junction of the greenstone and red slate of the 
 coal formation, and passes obliquely into the hill of green- 
 stone on the one side, and into the slate on the other in the 
 bed of the river. The principal vein is five or six feet in 
 diameter, and the matrix, toadstone, which is traversed, 
 in the direction of the vein, by several veins of sulphate of 
 barytes, which form saalhandes. The principal ore that 
 appears at the surface is the green carbonate, the pyritous 
 copper being rarer. 
 
 12. A similar vein in the same township. 
 
 About a mile below the vein just described, (down the 
 stream,) is another, which I am told is very similar and 
 therefore needs no description. In other places between 
 these veins, I have noticed, in the red slate, veins of the 
 green carbonate of copper, not more than a quarter of an 
 inch thick, while the walls are glazed so as to resemble pol- 
 ished steel ; constituting handsome specimens of the Slick- 
 i.m^ide of the Germans. 
 
 Mines, Veins, and Beds of Iron Ore. 
 
 13. Micaceous Iron Ore in Veins, i-n Montague. 
 
 Near the north line of the town, a little south west of the 
 mouth of Miller's river, a granitic hill of considerable extent 
 and elevation is traversed by veins of this ore in all direc- 
 tions; constituting one vast stock iverke. The principal vein 
 is nearly ten feet in diameter, and the gangue is quartz. I 
 do not see why this ore could not be profitably wrought. See 
 Journal of Science, Vol. 1, p. 438, where this ore is descri- 
 bed under the general name of specular oxide of iron.
 
 94 Geology, ^c, of the Connecticut. 
 
 14. Mint of Magnetic and Micaceous Oxide of Iron, in Haw 
 
 ley. 
 
 This exists in the north western part of the town, in beds, 
 in talcose slate. The foha of the slate are nearly perpen- 
 dicular to the horizon, and the principal bed of the ore va- 
 ries from six inches to three or four feet in thickness, and 
 numerous thin beds occur at the sides. The mine has been 
 opened twenty or thirty rods lortg, and thirty or forty deep. 
 The magnetic oxide is probably most abundant : but the 
 micaceous oxide has not till lately been wrought, through 
 an impression that it could not be smelted ! One or two tons 
 of it lie beside the mine ready for the mineralogist. I have 
 never seen any ore of this sort, that will bear any comparison 
 for beauty and richness of appearance with this. It has a 
 schistose, gently undulating structure, and plates of it may 
 be easily obtained, a foot in diameter, possessing a highly 
 glistening aspect. But it is no very easy matter to get at 
 this mine, on account of the extreme roughness of the coun- 
 try for several miles around it. 
 
 15. Mine of Magnetic and Micaceous Oxide of Iron, in Ber- 
 
 nardston. 
 
 This occurs in beds in talco-argillite, and is so similar to 
 the last described, that additional remarks are unnecessary. 
 I do not know to what extent it has been wrought. 
 
 16. Vein of Micaceous Oxide of Iron, in Jamaica in Vermont. 
 
 This exists in dolomite, and is very beautiful. It has been 
 used as a substitute for smalt, and answers well. I do not 
 know its extent. It is a few miles beyond the northern lim- 
 its of the map. 
 
 17. Mine of the Brown Oxide of Iron, in Salisbury in Con- 
 
 neciicut. 
 
 This, as well as the two following mines, occurs a consid- 
 erable distance beyond the limits of the map. I merely men- 
 tion them, however, because of their interesting nature j and
 
 Geology, ^c. of the ConnecticuU 95 
 
 In giving a list of the simple minerals, I do not intend to be 
 scrupulously confined to the region embraced by the map. 
 This mine is wrought in a bed in clay. For further partic- 
 ulars see Prof Silliman''s account of liiis ore, in the Journal 
 of Science, Vol. II. p. 212. 
 
 18. Mine of the same ore, in Kent, in Connecticut. 
 
 This is found, like the last, in a bed in clay. See Vol. 
 II. of the Journal of Science, p. 216. 
 
 19. Mine of Carbonate of Iron, in Kew-Milford, in Connecti- 
 
 cut. 
 
 This exists in a vein, in gneiss ; and its gangue is qaart/. 
 See Journal of Science, Vol. II. p. 226. 
 
 20. Bed of Bog Iron Ore, in Kew-Braintree, in Massstchn 
 
 setts. 
 
 This ore is not uncommon along the Connecticut; but I 
 have never examined a bed of it, except in New-Braintree, 
 in Massachusetts. It lies in a valley, in a country of gneiss, 
 only a few feet below the surface ; and has been explored 
 to a considerable extent. 
 
 21. Mine of Arsenical Cobalt, in Chatham, in Connecti- 
 cut. 
 
 It exists in a bed, in mica slate, varying in width from a 
 few inches to a few feet. The matrix is a mixture of horn- 
 blende and actynolite, in which the ore is disseminated. It 
 was explored several years since, and has been again open- 
 ed recently; the undertaking is now, however, abandoned. 
 Arsenical sulphuret of iron, arsenical nickel, and arseniate 
 of cobalt are found in this mine in small quantities. 
 
 r4
 
 90 Geology, &/■€. of the Connecticut. 
 
 22. Mine of Bismidh, Silver, Argentiferous a7id Common 
 Galena, Blende, Tungsten, Tellurium, JMagnetical and 
 Comrfion Pyrites, Spathic Iron, Native Sulphur, Pyrilous 
 Copper, ^c. in Huntington, in Connecticut. 
 
 The various minerals mentioned above, have been 
 found in a vein traversing gneiss, although it has yet 
 been explored only a few feet in depth. The gangue 
 is quartz. For a more particular description of this in- 
 teresting spot, see various articles by Professor Silliman, in 
 the first five volumes of the Journal of Science. 
 
 In the above enumeration several small and unimportant 
 veins of ore have been omitted ; and probably many impor- 
 tant ones are yet undiscovered In some instances I have 
 met with men who prx)fess to have found beds or veins of 
 ore, but will not disclose the spot, because they intend to 
 vender themselves independent by their discoveries. In- 
 deed, were the mineralogist to pay attention to all he will 
 hear on this subject in his travels, he would be led to sup- 
 pose that every town, and even every farm, is a rich reposi- 
 tory of metals. For he will often be told, how in such a 
 mountain the aborigines used to obtain iron, lead or silver; 
 or how, in such a place, the lightning frequently strikes, as 
 a certain indication of metallic ores; or how in such a place 
 the minrral rodzui/l work; and a thousand such mummeries, 
 by which honest but credulous men are frequently deluded, 
 and sometimes ruined. 
 
 List of Simple Minerals found along the Connecticut. 
 
 I have already remarked, that in giving this list, I should 
 not be confined precisely to the limits of the map; but 
 where an interesting mineral has been found a few miles be- 
 yond these, I shall notice it. I shall annex to each species 
 and variety, merely the localities and name of the discover- 
 er, except in cases where lam able to add some particulars 
 not heretofore published. To save all further trouble of 
 reference, I have taken the second edition of Cleaveland's 
 Mineralogy as a standard for names and arrangement. And, 
 indeed, I feel as if a better disposition of minerals could 
 scarcely be made, in the present state of the science, than 
 that excellent work presents.
 
 Geology, ^-c. of the Curnieclkut. 97 
 
 The species and sub-species are numbered in order 
 from first to last. The varieties also, whenever they occur, 
 are usually numbered. 
 
 1. Nitrate of Potash. Efflorescing on the soil under old 
 buildings, Sic. • 
 
 2. Sulphate of Barytcs. At Cheshire, Southington. Far- 
 mington, New-Stratford, and two miles from Hartford. (Sil- 
 liman.) Also at Berlin. {Percival.) Also at Hatfield. 
 (Gorham.) Also at Middlefield. (Eaton.) Also at South- 
 ampton lead-mine, at the Leverett lead veins, and at the 
 Greenfield copper veins. At the three last meniioned pla- 
 ces it is chiefly the lamellar variety. 
 
 3. Calcareous Spar. 
 
 1. Crystallised. At the Marble Quarry in Milford, in 
 rhombic crystals; also in the lead mine at Middletown. 
 (Silliman.) Also at the lead mine in Southampton, in lim- 
 pid and straw-colored crystals on galena and quartz. Forms 
 of the crystals. 1. A dodecaedron, composed of two six- 
 sided pyramids, applied base to base, {hog-tooth spar.). 2. 
 A short six-sided prism, terminated by three-sided pyra- 
 mids. 3. The same, with all the solid angles of the prism 
 truncated ; forming a crystal of twenty -four faces. Also, in 
 greenstone in Deerfield and Greenfield ; and in a coarse 
 limestone in Leyden, Conway, he. in rhombs. 
 
 2. Laminated. At Milford Hills. {Silliman.) Also, in 
 veins in greenstone, Deerfield. 
 
 4. Granular Limestone. At Milford Hill, embracing the 
 bed of Verd Antique Marble. {Sillunan.) In Wilmington, 
 
 Vt.? 
 
 5. Concreted Carbonate of Lime, 
 
 1. Calcareous Incrustations. In the Coal Formation in 
 Sunderland, &c.
 
 98 Geology, fyc. of the Connecticut. 
 
 6. Argentine. At Washington, Litchfield Co. {Brace.) 
 
 7. J\Iag7iesian Carbonate of Lime, 
 
 1. Crystalyzed. (Rhomb Spar.) Near New-Haven, with 
 abestus in Serpentine. [Stllinian.) Abundant at the Milford 
 Marble Quarry. Also at Middletiekl, in Soapstone. {Dew 
 ey.) Also at Southampton lead mine. {Eaton.) 
 
 2. Dolomite. At Washington and Milford Hills. {Silli' 
 man.) Also at Litchfield. {Brace.) Also at Middlefield. 
 {Dewey.) Also at Jamaica, in Vermont. {J. A. Allen.) 
 
 8. Brown Spar. At Leverelt, in a vein of galena, pyrites, 
 copper and blende, grouped in rhombic crystals on quartz; 
 the lamellae usually curved. 
 
 9. Fetid Carbonate of Lime. AtNorthford. {Silliman.) 
 
 10. Bituminous Carbonate of Lime. Near Middletown, 
 with Ichthyolites. {Silliman.) Also at Southington, in the 
 Coal Formation. 
 
 11. Phosphate of Lime. 
 
 I. Apatite. At Milford Hills. {Silliman.) 
 
 12. Filiate of Lime. Cubic and massive fluor spar occurs 
 in Huntington — also chlorophane in the same place. {Silli- 
 man.) Also at Middletown. in the lead, he. vein. {Brace.) 
 Also at Southampton lead mine, green and purple. {Gibbs.) 
 Also at Deerfield, crystallized in dodecaedrons.'' purple — in 
 a loose stone, which contained also a crystal of galena. {Coo- 
 ley.) Also at Putney, massive and grass green, forming a 
 vein in bastard mica slate. {Silliman.) Also at Westmore- 
 land, light green. {Hall.) Also at Conway, massive, light 
 green, in small quantities in a vein in mica slate. 
 
 13. Gypsum. In amygdaloidal greenstone in Deerfield, 
 in small quantities; "crystallized — white, and retaining its 
 water of crystallization.'' Found by Dr. Cooley, and de- 
 termint d by Professor Silliman. This has been already 
 mentioned in the geological part of this sketch.
 
 Geology., ^-c. of the Connecticut. 99 
 
 14. Sulphate of Alumine and Potash. (Alum.) In Ley- 
 deii, efflorescing on bastard argillite. Also in Conway, on 
 mica slate. 
 
 J 5. Common Quartz. 
 
 1. Limpid Quartz. At Grafton in Vermont, remarkably 
 pure. [Hall.) Also at Pia.nfield. {J. Porter.) Also in the 
 veins of lead, &c. at Soutbauipton and Leverett, and the 
 copper veins in Greenfield, in six-sided prisms. At the lat- 
 ter place it occurs with both the terminations perfect. Also 
 in veins in sienitic granite, at Northampton. Also in ge- 
 odes in greenstone at New-Haven, Berlin and Deerfield. 
 Also in veins and geodes from one to ten inches diameter, 
 in mica slate in Conway. The crystals are of every size 
 from one tenth of an inch to two inches diameter, and occur 
 in vast quantities. In the same town fragments of crystals 
 occur, as transparent as the quartz from Madagascar. 
 
 2. Smoky Quartz. At Torrington and Cornwall. (Brace.) 
 Also at Plainfield and Brattleborough ? amorphous. 
 
 3. Yellow Quartz. In crystals at the Southampton lead 
 mine; of a honey yellow, resembhng the Siberian topaz, 
 Th<? coloring matter appears to penetrate the crystals. Al- 
 so in small quantities at the lead mine in Leverett. 
 
 4. Rose-Red Quartz. At Southbury, very abundant. (Sil- 
 liman.) Also atChatham and East- Haddam. {T.D.Porter.) 
 Also at Deerfield ; a single specimen in alluvial soil. 
 
 5. Irised Quartz. At Plainfield. (J. Porter.) Also at 
 Lryden, in mica slate. 
 
 6. Milky Quartz. At Litchfield. {Brace.) Also at Cum- 
 mington and Plainfield. {J. Porter.) The specimens that 
 I have seen of this variety (and they are scattered abundant- 
 ly over the mica slate region west of Connecticut river,) are 
 rather poorly characterized, seeming to be intermediate be- 
 tween limpid and milky quartz.
 
 100 Geology, ^c. of the Connecticut, 
 
 7. Radiated Quartz. In the Southampton, Whately and 
 Leverett veins of galena ; in abundance. Also in Conway, 
 in veins and loose masses. 
 
 8. Tabidar Quartz. In s;reenstone, Deerfield — Lamellae 
 usually applied to one another by their broader faces, and 
 separating as thin as mica, but very brittle. Sometimes 
 they intersect and produce cells of various forms. Also in 
 Conway, in large loose masses among mica slate. Pieces 
 more than a foot in diampte'- have been noticed, having both 
 t^e structures above mentioned. The plates forming the 
 cells are sometimes covered on their broader faces with mi- 
 nute quartz crystals. In some specimens there is a gradation 
 from tabulir to common amorphous quartz; the folia becom- 
 ing less and less distinct, and finally disappearing. 
 
 9. Gramdar Quartz. At Vernon, Vermont, forming a 
 bed in argillite. {J. J. Allen.) 
 
 10. Pseudomorphous Quartz. At the Southampton lead 
 mine and in Deerfield greenstone — the impressions being 
 cubical. At the latter lo .ality also, a very curious variety of 
 this mineral occurs. The quartz is the common limpid 
 kind;, passitig, however, income parts, into chalcedony; 
 and it contains numerous cavities that diverge from a centre. 
 Their form is that of a four-sided, nearly rectangular prism, 
 generally a little flattened, and, of course, lessening to a 
 point at one end. Their length is from half an inch to four 
 inches. A complete sphere is seldom filled by them; usu- 
 ally not more than a quarter part of it; and at their outer 
 extremity they are so scattered as not to fill half the surface 
 of the sphere. I have sometimes observed these cavities 
 proceeding from different centres, crossing one another. 
 Although it is no uncommon thing to meet with these cavi- 
 ties, yet I have never found any mineral occupying them. 
 An interesting question then occurs ; by what were they 
 once occupied? The probability is, that it was some vari- 
 ety of zeolite. Yet no zeolite of this description has been 
 found in the greenstone in the vicinity. It exists in balls 
 perfectly filled; the crystals usually circular, and the con- 
 cretion never much larger than a musket ball. But the zeo- 
 lite, it is well known, does occur in radiated masses several
 
 Geology.) <J*c of the Conntcticut. 101 
 
 inches in diameter, the outer extremity of which presents 
 the form of the pri-m. I am rather disposed to beheve that 
 these cavities were once filled by a mineral not differing 
 much from the Thomsonite of Dumbarton in Scotland. 
 
 Some varieties of quartz occur along the primitive region 
 of the Connecticut that can hardly be referred to any of the 
 preceding Thus, there is a variety very abundant in beds 
 and tuberculous masses in mica slate and argillite, which 
 diff IS in nothing from limpid quartz, except that it is color- 
 ed cri nson red ; and perhaps it ought to be referred to fer- 
 ruginous quartz; but it diff rs from that commonly so cal- 
 led. Another variety is abundant every where, in large 
 rolled masses, of a reddish grey color when broken, with a 
 chonchoidal uneven fracture — the structure beini.' almost 
 granular, and the aspect considerably like hornstone. Anoth- 
 er variety, more rare, occurring in pudding stone, is of a 
 light blue color, and scarcely translucent; but it can hard- 
 ly be called the blue quartz of mineralogi?ts. Another va- 
 ritty is found in granite and in loose masses, and is nearly 
 black, and only semi-transparent. Another variety has a 
 tinge of \ellow — another of green, &,c. 
 
 16. Amethyst. At Wallingford, Farmington, Berlin and 
 East-Haven. Also at Mount Tom in East-Hampton. {Sil- 
 liman.) Also in greenstone, Deerfield, forming geodes of 
 a light purple; crystals from one tenth of an inch to an inch 
 in diameter. Also in Westminster, Vermont, in crystals an 
 inch and an half in diameter. 
 
 17. Ferruginous Quartz. At Litchfield. (Brace.) 
 
 18. Fetid Quartz. I have recently found this in several 
 places, from Woodbridge, near New-Haven, to Bellows- 
 Falls in New-Hampshire, a distance of one hundred and 
 iifty miles, in loose rolled masses. In the vicinity of Con- 
 way it is very abundant, and occurs crystallized in the com- 
 mon six-ssded prisms ; which are sometimes so flattened as 
 to be three times as broad as thick. In Conway it occurs 
 in veins in mica slate and granite ; less fetid, however, than 
 that which is found loose on the surface. It is traversed 
 by thin seams, or veins, apparently ferruginous; its color is 
 nearly milk white and its lustre a little resinous. In some 
 specimens the fetid odour is very strong. 
 
 /
 
 102 Geology, i^rc. of the Connecticut, 
 
 19. Chalcedony, 
 
 1. Common Chalcedony. At East-Haven, in greenstone. 
 {Silliman.) Also in the same rock at Southington, Far- 
 mington, Hadley, Sunderland, Deerfield, Greenfield, Gill, 
 and indeed, in almost every greenstone hillock and ridge 
 from New-Haven to Gill. Its color is light grey, deep grey, 
 brownish, yellowish and greenish grey; it occurs botryoi- 
 dal, mammillary, cylindrical and reniform, and is often of a 
 cloudy or milky appearance, and frequently, strongly trans- 
 lucent. 
 
 2. Cacholong. In greenstone, Deerfield. It is associated 
 with common chalcedony, and frequently, envelopes it, or 
 constitutes some of the bands of agates. Its color is milk 
 or yellowish white. 
 
 3. Carnelian. In greenstone, Deerfield. United with 
 common chalcedony and cacholong, into which it passes. 
 Its color is usually pale or yellowish red. It is not abundant. 
 Also at East-Haven. 
 
 4. Sardonyx? Some specimens of the carnelian in Deer- 
 field greenstone, being reddish yellow and oran2;e, appear 
 to belong to this variety; but it occurs in so small quantities 
 as hardly to be worth noticing. 
 
 Agate. This occurs at East-Haven and Deerfield ; and 
 as it is composed of varieties of chalcedony and quartz, this 
 seems to be the proper place to notice it. A description of 
 a part of the agates occurring in these localities has alre:ady 
 been given with sufficient minuteness in the American Jour- 
 nal of Science, and in Cioaveland's Mineralogy. But since 
 the publication of those accounts. Dr. Dennis Cooley has 
 discova-ed a new locality in the Deerfield greenstone, from 
 which ne has obtained specimens so mu( h superior to those 
 heretofore found that they deserve a particular notice. The 
 followii^^ is a description of specimens in his possession. 
 
 No. % Longer diameter of the face of the agate, nine 
 inches — shorter diameter, six inches Outer zone, i;reenish 
 chalcedony, half an inch broad. Second zone chalcedony,
 
 Gtology, ^-c. of ihe Conructicut. 103 
 
 a little tinged with red, a quarter of an inch broad. The cen- 
 tre is occupied by an amethystine <;eode of a light i)ur|)le. 
 )Veight of the whole agate, iwenty-ihree pounds. 
 
 No. 2. Face seven inches by four — Outer band, one 
 fourth of an inch wide, of yellowish red carnelian ; second 
 band greyish white chalcedony, one fourth of an inch. The 
 remainder of the space is occupied by a geode of limpid 
 quartz. The outer coat of carnelian is broken off from a 
 large part of this specimen, leaving bare the whi ish chalce- 
 dony, and it has a strong resemblance to the human crani- 
 um ; exhibiting similar protuberances and concavities. 
 
 No. 3. Face three inches in diameter — outer band ol yellow- 
 ish red carnelian — second do. chalcedony a little tinged with 
 red, one tenth of an inch — third do. cacholong, one tenth 
 of an inch — fourth do. light carnelian, one tenth of an inch. 
 The centre is occupied by common quariz, not forming a 
 geode. 
 
 No. 4. As it appears at one end : Diameter of the face 
 three inches — outer zone three fourths of an inch thick, of 
 yellowish green chalcedony — second do. carnelian, one 
 fourth of an inch — third do. quaitz, having a greasy aspect 
 — fourth do. dark grey translucent chalcedony, a mere line 
 in thickness — fifth do. quartz or milk colored chalcedony, 
 one tenth of an inch — sixth do. dark grey chalcedony, a line 
 broad — seventh do. quartz, one fiftieth of an inch — eight do. 
 dark grey chalcedony, a line broad — ninth do. quartz, one 
 tenth of an inch — tenth do. chalcedony, a line broad — elev- 
 venh do. quartz, one fiftieth of an inch — twelfth do. a line 
 of chalcedony — thirteenth do. quartz, one thirtieth of an 
 inch — fourteenth do. a line of chalcedony. The centre is 
 occupied by limpid quartz. This is a fortif cation agate, 
 and the parallelism of the several bands is most exactly 
 preserved, and the angles are perfect. Viewed on a face 
 at right angles to that above described, this specimen exhib- 
 its a striped or ribband agate. 
 
 No. 5. Made up of an almost countless number of dark- 
 er and lighter colored bands of whiteand grey chalcedony 
 — two or three small agates appearing on the same face. 
 
 15 
 
 /
 
 104 Geologi/, c^c. of the Connecticul. 
 
 This appears \q be a real ch alec don ij x ; and such specimens 
 are not uncommon. 
 
 No 6. Fortification and Etjrd Agates, in the same speci- 
 men. One of tlie later is an inch in diameter, and has six 
 or seven zones of hghtrr and darker c!ialcedony and one of 
 carnelian, enveloping a nucleus of light blue chalcedony. 
 
 These specimens seem to want nothing but a polish to 
 make them equal to any in the splenrlid cabinet in New- 
 Haven. The rock in which they occur i- not strictly amyg- 
 daloidal, but contains only a few large cavities; and so firm- 
 ly are the agates fastened into iheir bed that one is often 
 obliged to brt^ak them out by piecemeal ; thus ruining the 
 most superb specimens. The larger ones are not very abun- 
 dant. The rock, however, has not been penetrated very 
 far. 
 
 20. Siliceous Sinter. At East-H -ddam, in gneiss and in- 
 crusting raica siate. (T. D. Porter and Webster.) 
 
 21. Opal. "Common opal has been found in Litchfield, 
 though rarely." (Brace.) 
 
 22. Flint. Near Nevi'-Haven and in Woodbridge, in roll- 
 ed masses. [Silliman.) 
 
 23. Hornslone. At Litchfield. (Brace.) At the Southamp- 
 ton lead mine ; also in Conway. Also in greenstone at 
 Southington and Deerfield At the latter place it occau's in 
 nodules often four or five inches in diameter. Its colors are 
 grey, green, black with a tinge of red, and dark blue. Its 
 fracture is sometimes a little chonchoidal and glistening, 
 sometimes dull and splintery; and it is scarcely translucent 
 at the edges. Some specimens considerably resf-mble sili- 
 ceous slate, and otliers appear like prase. But Professors 
 Silliman and Dev.ey (the latter of whom has examined it 
 chemically,) agree in calling it hornstone. Also in Sunder- 
 land in greenstone, in narrow veins — well characterised. 
 
 24. Jasper. Near New-Haven in rolled masses. (Gibbs.) 
 Also at Cummington on the banks of Westfield river- (/. 
 Porter.) Also on the banks of Deerfield river in Deerfield,
 
 Geology, ^~c. of the Connecticut. 105 
 
 and in Conway, Leyden, &£c. in rolled fragments, red, black 
 and yellow. 
 
 25. Corundum. At Litchfield, massive and in six-sided 
 prisms, imbedded in niHSsive sappar. {Brace.) 
 
 26. Cycmite. At Litchfield, Harwinton, Watertown and 
 near New-Haven. (Stlliman.) At tne former place a mass 
 of this mineral, associated with talc, sulphuret of iron and 
 corundum, is supposed to weigh one thousand five hundred 
 pounds. (Brace.) Also at Middle-Haddara. (Eaton.) Al- 
 so at Chesterfield, Mass. in loose masses in mica slate; 
 where its bladed or imperfect prisms are two feet long. 
 (Hunt.) Also at Granville. (Drw^y.) Also at Plainfield. 
 (./. Porter.) Also at Grafton, Vermont, and Charlestown, 
 New-Hampshire. (Hall.) Alr^o at Bellov\s Falls. (Silli- 
 niaa.) Also at Deerfield, in mica slate. (Williams.) 
 
 27. Slaurotide. At Bolton, East-Hartford, Beacon-Hill, 
 Litchfield, Harwinton and Chatham. (Silliman, Brace, Ea- 
 ton and Woodhridge.) Also at Cummington. (/. Porter.) 
 Also at Bellows Falls. (Hall.) The range of mica slate in 
 which this minei'al is found in Bolton, Chatham, &:c. extends, 
 with little interruption, into New-Hamj'shire and Vermont, 
 at least as far as Bellows Falls; and its aspect is very simi- 
 lar throughout, and scarcely a mile of the distance is it want- 
 ing in stam'otido; or rather, wherever 1 have crossed it, (in 
 perhaps fifty places ) this mineral occurs ; as in Vernon, 
 where it is in vast quantities, in North-Will)raham, Ludlow, 
 Shutesbury, Leverett, Northford, Hinsdale, Chesterfield, 
 Putney, Westminster, Sir. In Chesterfield, New-Hamp- 
 shire, Dr. J. A, Allen found crystals an inch and one fourth 
 in diameter, and two inches and an half lony, in the valley 
 south-west of the meeting-house. A raii^e of similar mica 
 slate extends through Chesterfield, Mass. into Cummington, 
 Plainfield, Hawley, kc. and here also stuurotide occurs in 
 abundance. In Chesterfield I noticed a mica slate rock, 
 two or three feet thick, containing seven or eight distinct 
 layers of this mineral. 
 
 28. Pinite. At Haddam. in mica slate and p'anite. (Sil- 
 liman and Webster.) Also at Bellows Falls. (Hall.)
 
 105 Gco/oiry, 4'-<"- of the Connecticut. 
 
 29. Chrysoberyl. At Haddam, on both sides of the river, 
 ill six-sided prisms and six-sided tables, in granite. (Cribbs.) 
 
 00. Zircon. At Sharon, Litchfield county, in quartz. 
 {Silliman.) Also at Brinitield, in gneiss. (Eaton.) 
 
 31. Siliceous Slate. 
 
 1. Basnnife. Sometimes found in alluvial soil on the 
 banks of Deerfield river; but perhaps brought thither by 
 the aborigines, who made use of this and of jasper for barbs 
 to their arrowsand pikes. 
 
 32. Piichstone. Near New-Haven. {Silliman.) 
 
 33. Mca. 
 
 1. Laminated. At Leverctt, Alstead, &c. 
 
 2. Lamellar. At Woodbury it is violet. (Silliman.) Also 
 at Goshen, Mass. yellownsh green and violet, and some- 
 times in rhombic tables. (Gibbs.) Of the same colors at 
 Bellows Fails, in granitic veins. (Silliman.) Most of the 
 mica in the granitic veins in Conway, Ashlield, Williams- 
 burgh, Chesterfield, Sic. is straw yellow, sometimes rose- 
 red, and in these veins it exists in excess. It occurs in 
 these and other towns also, in granite of a smoky or nearly 
 black color. 
 
 3. Pri.wiaiic .Mica. Near Watertown. (Silliman.) A\ 
 Litchfield. (Brace.) 
 
 34. Shorl. 
 
 1. Common Shorl. At Haddam, in six-sided prisms, ter- 
 minated by threfe-sided pyramids. (Gibbs and Webster.) It 
 occurs in almost every town in the primitive region along 
 the Connecticut. Localities where it is found abundant, 
 or beautiful, are Pelham, Shutesbury, Orange and Brattle- 
 borough. Ai the latter place it is found abundantly neaj- 
 the centre of the town in mica slate or hornblende slate : 
 and also near the north line of the town (mentioned in 
 Cleavcland's Mineralogy as occurring in Dummcrston.) it
 
 Geology, ^c. of the Connecticut. 107 
 
 exists in crystals half an inch in diameter and often four or 
 five inches long, sometimes terminated hy three-sided pyr- 
 amids, in common white quartz. The contrast renders the 
 specimens quite beautiful, and one large loose mass lies on 
 the surface nearly two feet in diameter, which would be an 
 ornament to a mineral cabinet. 
 
 2. Green Tonrmalinc. At Chesterfield and Goshen, Mass. 
 (Gibbs.) These interesting localities have been so well 
 described by Col. Gibbs, as to render any farther remarks 
 unnecessary. (Am. Jour. Vol. I. p. 346.) 
 
 3. Indkolite. At Chesterfield and Goshen. (Gibbs.) 
 At Bellows Falls. (Silliman.) At Hinsdale, New-Hamp- 
 shire, in granite, in great abundance. (J. A. Allen.) This 
 locality is found most readily by taking the road from Hins- 
 dale to Winchester. 
 
 35. Ruhellite. At Chesterfield and Goshen, Mass. (Gibbs.) 
 Sec his account in the Journal of Science, as above cited. 
 
 3G. Feldspar. 
 
 1 . Common Feldspar. Near Haddam, greenish and trans- 
 lucent. (McEwcn.) In the same vicinity it is of a light flesh 
 color, and in large masses in granitic veins and beds. Also 
 of the same color in pudding-stone, Deerfield. Also in large, 
 bluish, imperfect crystals, in granite, Leverett. It occurs, 
 of course, abundantly in all that part of the map colored as 
 granite, gneiss and sienite. 
 
 2. Adularia. At Haddam. (T. D. Porter.) At West- 
 Springfield and Southampton lead mine. (Waterhouse.) At 
 Brimfield. (Eaton.) 
 
 3. Siliceous Feldspar. (Gibbs.) At Chesterfield, Mass. 
 and Haddam. (Gibbs.) Also at Goshen — a new varicty^j 
 discovered by Dr. Hunt. 
 
 37. Precious Emerald. At Haddam ? For a discussion of 
 the subject whether this mineral exists in the United States, 
 see Cleaveland's Mineralogy. Vol. l.p. 341.
 
 108 Geology, fyc. of the Connecticut, 
 
 38. Beryl. At Brookfield, Huntington and Haddam. {Sil- 
 liman.) Also at Litchfield. (Brace.) Aho at Chatham. 
 (Mather.) Also at Chesterfield, Mass. and Goshen. (Gibbs.) 
 At Chesterfield and Haddam the crystals are sometimes 
 from nine to twelve inches in diameter. At Goshen some 
 are rose-colored. I found some crystals of beryl four or 
 five miles north of the centre of Haddam. 
 
 39. Garnet. At Haddam — four inches diameter. (Silli- 
 man.) Also at Tolland, nearly rose-red. (Webster.) Also 
 at the cobalt mine, Chatham, in mica slate, crystallized in 
 rhombic dodecaedrous, or rather six-sided prisms termina- 
 ted by three sided pyramids — the prisms often considerably 
 elongated — color pale red — size that of a common musket 
 bullet. Also at Plai'nfield, in limpid quartz, in trapezoedrons, 
 or having at least as many as twenty-four sides — color of 
 the mass nearly iron black. Found by J. Porter. Also 
 at the same place in talco-micaceous slate, in dodecae- 
 drons; color brownish red; size of a pea. Also at the 
 same place, in dodecaedrons, truncated and striated on all 
 their edges by hexaedral faces ; presenting thirty-six faces 
 in the whole — color dull red — size of a common bullet. 
 Also at the same place in talcose slate, in dodecaedrons of 
 the same color, sometimes two inches in diameter. Also at 
 Chesterfield, Mass. with sappar, in trapezoedrons ; color 
 light rose-red — size of a pea. Also in hornblende and mi- 
 ca-slate, in Conway and Deerfield ; color nearly black — 
 crystals dodecaedrons — sometimes as large as a common 
 bullet. Also in Conway, a loose mass, almost wholly made 
 up of small black garnets in dodecaedrons — size less than 
 one tenth of an inch in diameter, and with scarcely any dif- 
 ference in the size of hundreds. Also at Marlborough, Ver- 
 mont, one mile south of the meeting-house, in dodecaedrons 
 of a cherry-red, in chlorite slate; but hardly the precious 
 garnet. They occur at this spot in immense quantities, 
 and beautiful specimens may easily be obtained. A hun- 
 dred other localities of the common garnet tnight be men- 
 tioned ; since it occurs in all our primitive rocks: but the 
 most interesting have been noticed. 
 
 1. Pyrope. At Brimfield, Mass. in granite, the feldspar of 
 *'hi^h h li^ht green — in rounded irregular masses of a del-
 
 Geology, &fc. of the Coymectintt. 109 
 
 icate poppy red, much re?cmbling some varieties of (he ru- 
 by. ''It scratches crystaliized quartz," says Professor 
 Dewey, ""and melts, rather hardly, into a dark cnameJ.'' 
 Found in digginj^ a well- 
 
 2. Colophonitc. At Conway ? 
 
 40. Magnesian Garnet. At Haddam. (Vide Cleaveland's 
 Min. Vol. 2. p. 777.) 
 
 41. Epidote. At Milford Hills, in primitive greenstone. 
 (Silliman.) Also at Litchfield and Washington, in gra[)hic 
 granite and sienite; crystallized. (Brace.) Also at Had- 
 dam, crystallized. Also at Tolland. (Webster.) Also at 
 Athol, Worcester county, Mass. in prismatic hiaded crys- 
 tals, associated with black radiated schorl and hornblende. 
 Also in Shutesbury, in small crystals in gneiss. It occurs 
 also in a great many other places, disseminated in various 
 rocks, and not very interesting. 
 
 1. Zoisite. At Haddam. (Webster.) Also at Wardsbo- 
 rough, Vermont, in much compressed, greenish grey, pris- 
 matic crystals: sometimes a foot long and one or two inch- 
 es wide. (Dczvey.) Discovered by Dr. J. A. Allen. Also 
 at Leyden, Brattlcborough and Westmoreland. (Hall.) 
 
 2. Arenaceous Epidote. At Haddam. (Webster.) Also 
 at Shutesbury, Leyden, Shelburne, Buckland, Whately, 
 Belchertown, Monson, and a great number of places, in 
 hornblende and greenstone slate. 
 
 42. Prehnite. Near New-Haven, in secondary green- 
 stone, in radiated masses, or in veins. Also at Woodbury, 
 in the same sort of rock, in mammillary, botryoidal and al- 
 most globular masses. (Silliman.) Also between Simsbury 
 and Wintonbury, in mammillary masses in greenstone. 
 (Hayden.) Also in Deerfield, Greenfield, and, indeed, in 
 almost every part of (he secondary greenstone ranges from 
 New-Haven to Gill; in all the forms mentioned above. In 
 Deerfield the radiated masses sometimes contain pyritous 
 copper. They occur there, also, on pseudomorphous quartz, 
 having evidently been formed since the decomposition of 
 the crystals originally occupying the cavities. In the same
 
 110 Geology, ^c. of the Connecticut. 
 
 place, 1 have found prchnite crystallized in t^roups on chal- 
 cedonv; but could not determine the form of the crystal. 
 Also near Bellows Falls in primitive rocks. I saw speci- 
 mens in the cahinet of Dr. Wells; but was not informed of 
 the precise locality: yet the mica attached to the speci- 
 mens indicated their detachment from the older classes of 
 rocks. 
 
 43. Stilbite, At Woodbury, well characterized. (Silli- 
 man.) Also at Deerfield in secondary greenstone ; usually 
 associated with chabasie. Its crystals appear to be right 
 prisms, whose bases are rhombs with angles of about 60' 
 and 120°. They rarely exceed one tenth of an inch in 
 their longest direction. They are frequently grouped so 
 as to become mere foliated masses. The lustre of the fo- 
 lia is pearly, and they are usually a little curved; color 
 white. On hot coals it whitens and before the blow-pipe 
 intumesces and melts into a white spongy enamel. It is but 
 rarely met with. 
 
 44. Zeolite. Near New-Haven it is found in secondary 
 greenstone, crystallized, or radiated, or mealy. (Silli/nan.) 
 Also at Deerfield, in radiated librous masses, sometimes as 
 large as a musket bull(;t,or morerarely an inch in diameter. 
 
 45. Lmimonite. In secondary greenstone, also in loose 
 rolled masses of pudding-stone near New-Iiaven. {Silliman.) 
 
 4G. Analcime. At East-IIaven, with chalcedony and 
 agates. {T. D. Porter.) Also at Meriden, Connecticut. 
 {Silliman.) Also at Deerfield, usually in laminated or ra- 
 diated masses, which are reniform, cylindrical and nearly 
 spherical. Very rarely in trapezoidal crystals — color white, 
 grey and flesh-colored. Associated w^ith calcareous spar, 
 quartz, chalcedony, Szc. and frequently eflfervesces a little 
 with the acids. 
 
 47. Chabasie. At Deerfield, in cavities and seams in se- 
 condary greenstone; usually crystallized in transparent, or 
 brownish, or yellowish crystals; presenting the primitive 
 form, from one twentieth to one fourth of an inch in diame- 
 ter, insulated and grouped on limpid, psendomorphous and
 
 Geology, ^c. of the CGuncclicvt. Ill 
 
 tabular quartz, chalcedony, balls of zeolite, &c. Hundreds 
 of specimens have been obtained at tliis place. 'J^o procure 
 them, however, requires much labour. 
 
 48. Apophyllite. Near Saybrook, Connecticut. (Gibbs.) 
 
 49. TremoUtf. At Milford, Washington, Goshen, Canaan, 
 (Conn.) &;c. in dolomite and granular limestone. (Silliman.) 
 
 A mineral is found at Le}' den in great quantities, associated 
 with quartz, limestone &.c. and sometimes forming the gangue 
 of the red oxid of titanium ; the same occurs also at West Ha- 
 ven or Orange in hornblende — also at Leyden . at Colrain . 
 at Shelburne . at Conway at Goshen , (Mass.) at Guil- 
 ford and Bratlleborough . Vt. and in various instances, in 
 vast abundance: this mineral has generally been called 
 tremolite, and sometimes zoizile, but it is probably scapohte. 
 
 50. Asbeslus. At New-Haven and Milford, in serpentine, 
 very beautiful. (Silliman.) Also at Pelham, Mass. where it 
 occurs with serpentine and talc. 
 
 Amianthus. At New-Haven and Milford. Also at Wash- 
 ington. (Silliman.) 
 
 51. Augite. At Litchfield in dolomite — the whitish varie- 
 ty. (Brace.) Also atBrookficId and Washington in dolomite. 
 (Eaton.) Also at Goshen, Mass. in granite, in flattened 
 greenish gray prisms, sometimes eight inches long and two 
 inches wide. This locality is one mile north of the meet- 
 ing house, on the road to Ashfield. Also at Deerfield, in 
 secondary greenstone, associated with quartz and calcareous 
 spar, either in irregular veins or imperfect crystals — colour 
 black — not abundant. 
 
 1. Sahlite. Near New-Haven in serpentine rocks belong- 
 ing to the formation of verd-antique marble. (Silliman.) 
 
 52. Common Hornblende. This, of course, occurs in great 
 quantities as a constituent of several rocks marked on the 
 map ; indeed, it may be found in a good degree of pu- 
 rity almost every where along the Connecticut, either in 
 place or in rolled masses. 
 
 16
 
 112 Geologj/, fyc. of the Connecticut. 
 
 1. Ldinrllar Hornblende. Good specimens are found in 
 Holland Mass. (Eaton.) Also in Leverelt, Sunderland, Con- 
 way, &c. of a black colour, in Shutesbury it is green. 
 It is found in sienitic granite and gneiss, in scales tbal are 
 easily mistaken for black mica. 
 
 2. Fibrous Hornblende. At Leyden, the fibres very fine. 
 Also near Bellows Falls, extremely beautiful, associated with 
 quartz. Also in Slielburne, Conway, Go.^hen, &i.c. in mica 
 slate, in large and broad fibres or lamellae. 
 
 3. Fasciculile. This is composed offibres, or rather in many 
 instances, of lamellae, frequently more tlian ^\ of an inch 
 broad, diverging at both ends, so as to occupy usually, as many 
 as 60° of a circle. These lamellae are commonly inserted 
 perpendicularly to the folia of the slate in which they occur, 
 and are applied to each other by their broader faces, being 
 bent outwards on both sides, somewhat like a bow, and pre- 
 senting elegant and very perfect fascicles. Tne fibres or 
 lamellae, scarely, if ever, cross one another; y-^^t some- 
 times they diverge in nearly straight lines, and sometimes 
 are so much curved as to resemble very exactly a sheaf 
 of grain when standing erect. (See Plate 9,) The figure in 
 the plate does not give a representation more regular or dis- 
 tinct than many of the most perfect specimens present. The 
 length of the fibres or lamellae varies from one to four inch- 
 es. It is found 'v\ mica slate and talco-micaceous slate in 
 Hawley. Plainfield. and Conway. Probably this variety is 
 comprehended under Fibrosis Hornhhnde by Cleaveland ; 
 and perhaps specimens as perfect as those described above 
 are not unfrequent. But so exact and striking an instance 
 do these exhibit of the fascicular structure of minerals, that 
 I could not resist the temptation to denominate them Fasci- 
 culite. 
 
 4. Hornllcndr Slatr. For aa account of this, see the Geo- 
 logical part of this sketch. 
 
 53 Act^piolite, At Saybrook, and near N. Hav'en in ser- 
 pentine. (Silliman.) Also at Litchfield. (Brace.) Also at 
 Middlefield. (Dewey.) Also at Hawley. (Eaton.) Also at 
 Cummington. (J. Porter.) Also at Windliam in compressed
 
 Geology, ^c. of the Connecticut. 113 
 
 four sided prisms, in steatite and talc ; the specimens su- 
 perb. (Hall.) Also at Chatham Ct. near the bank of the 
 river opposite the upper ferry in Haddarn, in an enormous 
 granitic vein; associated with black schorl, magnetic oxide 
 of iron, &,c. Also at Belchertown. Also at Shutesbury in 
 gneiss. Also at New Salem in acicular crystals in chlorite. Also 
 at New Fane, where it was discovered by Dr. J. A. Allen. 
 It occurs in steatite in four sided, sometimes very perfect, 
 sometimes flattened and striated crystals, five or six inches 
 long, often half an inch broad, generally radiated, sometimes 
 curved and crossing one another. The colour is a dark 
 beautiful green, and the specimens are very elegant. 
 
 54. Anthophillite. It is said to have been found near 
 Say brook (Cleaveland's Mineralogy.) 
 
 55. Diallrige. In serpentine rocks near New-Haven — 
 well characterised. (Hall.) Also in Conway ? in granite. 
 
 56. Made. At Bellows Fal's Croyden, Cornish, Charles- 
 town, Langdon and Alstcad in argillite. (Hall.) According 
 to Mr. Nultall, the foliated mineral occurring so abundantly 
 in the mica slate in Chesterfield, Plainfield, Hawley, Heath. 
 &,c. being usually inserted in small bronze coloured plates, 
 nearly at right angles with the folia of the slate, may be 
 made. 
 
 57. Serpe7itine. 
 
 1. Precious Serpentine. At Milford, in nodules or irregu- 
 lar masses in primitive limestone. (Silliman.) 
 
 2. Common Serpentine. In extensive beds and variously 
 blended with limestone at Milford and New-Haven, forming 
 the Verd Antique. (Silliman.) Also at Westfield in granite. 
 (Eaton.) Also at Middlefield, associated with steatite. (Dew- 
 ey.) Also at Grafton, Windham and Putney, Vermont, in 
 large insulated masses weighing many tons. (J. A. Allen.) 
 Also at Pelham Mass. in a large loose mass penetrated by 
 asbestus and associated with talc. Also at Leyden, Shel- 
 burne, Deerfield, &.c. in small rolled masses. 
 
 58. Tafr.
 
 I 14 Geology^ ^'C. of the Conncciicid. 
 
 1. Common Talc. At Haddam, Litchfield and Southamp- 
 ton. (Cleaveland) Also at Cummington in steatite. (J. Por- 
 ter.) Also at Middlefield in steatite. (Dewey.) Also at 
 Windham in steatite — laminae very large and beautiful. (Hall.) 
 Also in New Fane in steatite — specimens laminated and el- 
 eaant. (J. A. Allen.) Also at Pelham, associated with ser- 
 jientine and asbestus. Also at Rovve. 
 
 2. Induraled Talc. At Milford marble quarry. (Silli- 
 man.) 
 
 3. Scaly Tide. At Windham and New Fane. (J. A. 
 
 Allen,) 
 
 .59. Steatite. 
 
 1. Common Steatite. Near New-Haven and at Litchfield. 
 (Cleaveland.) Also at Middlefield connected, with serpen- 
 tine and mica slate, and crystallized in six sided prisms ter- 
 minated by six sided pyramids. (Dewey.) Also at Grafton 
 and Windliam. (Hall.) Also at New Fane and Marlbo- 
 rough. (,J. A. Allen.) Also at Savoy and Cummington (J. 
 Porter.) Also at Westminster, Vermont, where, as well 
 as at Grafton, it is wrought into aqueducts and answers a 
 valuable purpose. Also at New Salem forming a bed in 
 gneiss. 
 
 2. Potstone. At Grafton, Vermont, in large quantities. 
 (Hall.) 
 
 60. Chlorite. 
 
 1, Common Chlorite. Near New^-Haven, penetrating 
 quartz and calcareous spar, and in greenstone. (Silliman.) 
 Also at Saybrook, crystallized. (T. D. Porter.) Also at 
 Wardsborough, Vermont, in dark green folia. (Dewey.) 
 Also at Halifax, Leyden, Conway, &,c. foliated. Also at 
 Miller's Falls in Montague penetrating milk white quartz. 
 Also at New Salem. Also in greenstone amygdaloid at 
 Deerfield, Greenfield, Gill, kc It fills two thirds of the 
 cavities in some varieties of greenstone, and to the naked 
 eye has a radiated aspect, but Professor Dewey remarks,
 
 Geology^ ^c. of the Connecticut. 115 
 
 iJiat it does not appear to be radiated under a magnifier, 
 great or small ; but to consist of folia curiously arranged 
 often with no regularity and their length somewhat greater 
 than their breadth." 
 
 2. Chlorite Slate. For an account of this, see the map 
 and the Geological part of this sketch. 
 
 3. Green Earth. A part of the chlorite described above 
 in the amygdaloid in Deerfield, &,c. appears to belong to this 
 variety. 
 
 61. Argillaceous Slate. 
 
 1. Argillite. 
 
 2. Shale. 
 
 "3. Bituminous Shale. For a description of these minerals 
 ihc reader is referred to the Geological part of this sketch. 
 
 62. Claystonc. This is found in rolled peices in the bed 
 of Connecticut river below where it cuts through the coal 
 formation at Gill ; and probably this mineral is worn from 
 thence by the water. The pieces frequently occur in the 
 form of a prolate spheroid, sometimes flattened, even to the 
 shape of a wheel, and sometimes assuming shapes bearing a 
 resemblance to the sculptured images of Persia and India. 
 It is opaque — colour, light gray — scarcely adheres to the 
 tongue, and yields a slight argillaceous odour — fracture dull 
 and uneven, a little conchoidal — easily scratched with a 
 knife and even by the finger nail ; yet its particles scratch 
 iron. It does not effervesce with acids. 
 
 6:3. Clay. 
 
 1. Porcelain Clay. At Washington Ct. in small quantities. 
 (Cleaveland.) Also at Plainfield (Silliman.) Also at Con- 
 way and Leyden in small quantities. 
 
 2. Potters Clay. In the older alluvion along the Connect- 
 icut, abundant.
 
 116 Geology, <^-c. of the Connecticut. 
 
 3. Loam. In the newest alluvion along the Connecticut. 
 
 4 Fuller'' s Earth. At the bed of iron ore in Kent. (Silli- 
 inan.) 
 
 64. Sulphur. This occurs pulverulent in small quantities 
 in mica slate, in Warwick, Shelburne, Conway, &.c. Per- 
 haps it proceeds from the decomposition of some sulphuret. 
 
 65. Graphite. At Cornwall, Connecticut. (Brace.) Also 
 at Tolland. (Webster.) Also at Hebron and Sharon. 
 (Cleaveland.) Also between Sturbridge and Holland, 
 
 Mass. 
 
 66. Coal. At Durham, Middletown, Chatham, Southing- 
 ton, Berlin, Suffield, Enfield, Somers, Ellington and South 
 Hadley. (Silliman.) Also in the drift, of the Southampton 
 lead mine. From some of these localities, the coal is high- 
 ly bituminous, in others scarcely so at all. 
 
 C7. Lignite. 
 
 1. Jet. At South' Hadley. (Gibbs.) 
 
 68. Peat. In small quantities at Leveiett, Mass. 
 
 69. Native Silver. At Huntington in the bismuth mine. 
 Also at West River Mountain, Chesterfield, New-Hamp- 
 shire. (Silliman.) After the remarks and explanations giv- 
 en by Prof. Silliman. (Am. Jouru. Sci. Vol HI. p. 74. 
 note,) no reasonable doubt can remain concerning this last 
 locality. 
 
 70. Sulphuret of Silver. In Connecticut it is said to have 
 been found. (Cleaveland's Mineralogy.) 
 
 71. .Yative Copper. At Bristol, Connecticut, in a vein 
 with the red oxide of copper. (Gibl)S.) .Also on the Ham- 
 den hills, a mass of about ninety po'mHs, adhering to the 
 rock. Also twelve miles from New-Haven near the Hart- 
 ford turnpike, a mass of six poimds in alluvial soil. (Silli- 
 man ) Also at VVhately, Mass. in geest, on the limit be- 
 tween the primitive and alluvial soil, and about five miles
 
 Geology, ^c. of the Connecticut. 117 
 
 from secondary greenstone or the coal formation. The 
 piece weigiis seventeen ounces and very much resembles 
 the last mass above described, exhibiting imperfect rudi- 
 ments of octaedral crystals on the surface, and being encrust- 
 ed by green carbonate of copper. The cavities alao con- 
 tain a very little red oxide of copper. 
 
 72. Sulphuret of Copper, Near New-Haven, at Simsbury 
 mine, &:c. (Silliman.) 
 
 73. Pyritous Copper. At Cheshire, Simsbury, he. (Silli- 
 man.) Also at the Southampton lead mine, where it occurs 
 amorphous and crystallized in regular tetraedrons which are 
 insulated on calcareous spar. For the specimens contain- 
 ing these crystals, I am indebted to Dr. David Hunt. Also 
 at the Leverett lead mine amorphous. Also in greenstone, 
 Deerfield. Also at Greenfield in veins, in greenstone and 
 sandstone. 
 
 74. Variegated Pyritous Copper. This occurs sparingly 
 disseminated in calcareous spar in sandstone of the coal for- 
 mation. In the island in the middle of Connecticut river at 
 the falls in Gill. 1 am indebted to Prof. Dewey for the de- 
 termination of this mineral. 
 
 75. Antimonial Gray Copper. Near Hartford, in the red 
 sandstone formation, (coal formation ?) (Maclure.) 
 
 76. White Copper. At Fairfield ?* Connecticut. (Silli- 
 man.) 
 
 77. Red Oxide of Copper. At Bristol, in a vein with na- 
 tive copper. (Gibbs.) Also with native copper in the green- 
 stone mountains extending northerly from New-Haven. 
 (Silliman.) 
 
 78. Green Carbonate of Copper. At Greenfield, near the 
 Falls in Gill, in two veins with pyritous copper, in considera- 
 ble abundance near the surface. It is amorphous and even 
 earthy. 
 
 * There is great rpason tobpliere that this locality is not correct. — Editor.
 
 118 Geologi/, Sfc. of the Connecticut. 
 
 1. Fibrous Malachite. At Cheshire, &c. in small but good 
 speciinens. (Silliman.) 
 
 79. Arsenical I -on? or Arsenical Sulphiiret of Iron ? At 
 Gill in a loose mass weighing several pounds. Found by 
 Dr. Alpiieus Stone. 
 
 80. Sidphurei of Iron. (Pyrites — Iron Pyritr-s.) This is 
 found in every town and in almost every rock along the 
 Conn- cticut ; as in the bituminous shale at Westfield and 
 Sunderland, compact and aninphous; also in other rocks 
 of the coal formation. Also at Plainfield, disseminated in 
 limpid quarlz. Also atHawley, compact and unmixed with 
 any gangue Also at Hahfax, Vermont, in an immense 
 mass found in digging a cellar. Also with micaceous oxide 
 of iron ?.t Montague. Al-o at the Southampton lead mine, 
 beautifi'lly crystallized in octaedrons which are truncated in 
 all their angles. It is grouped or insulated on crystallized 
 quartz, and the crystals are about as large as a small shot, 
 yet perfectly distinct and well marked. 
 
 81. Magnetic Sulphurcl of Iron. At Brookfield, abundant 
 in granite. Also at Huntington with bismuth, &.c. (Silli- 
 man.) Also near V^^oodbury in gneiss. (Eaton.) 
 
 82. Arsenical Sufphuret of Iron. At Derby Middle- 
 lown, and the Chatham Cobalt mine. (Silliman.) AlaO at 
 Leicester, Mass. in gneiss. (Dewey.) 
 
 83. Magnetic Oxide of Iron. At Somerset, Vermont, 
 in beds from one inch to two feet thick, in mica slate. (J. 
 A. Allen.) At Chatham, near the bank of the river, oppo- 
 site the upper ferry iu Haddam, in a granite vein with 
 schorl, actynolite, garnets, he. The crystals are octae- 
 drons, well defined, and often nearly an inch in diameter. 
 Also at Plainfield, Shelburne, Athol, Shutesbury, he. in 
 smaller octaedrons in mica slate and gneiss. Also in beds 
 in talcose slate at Ilawlcy. Also in beds in Bcrnardstown. 
 
 1. Iron Sand. At West I Javcn beach abundant. (Silli- 
 man.) Also on the beach near the Li^ht House in East 
 Haven in great abuudance. Also a little below Turner's 
 Falls in Gill, on the southeast baidv of Connecticut river.
 
 Geology, ^c. of the Connecticut. 119 
 
 84. Specular Oxide of Iroyi, Sometimes covering quartz 
 and other minerals ; as at New Fane and Leyden ; but not 
 abundant. 
 
 85. Micaceous Oxide of Iron. Ai Jamaica, Vermont, in 
 dolomite ; very handsome. (/. A. Allen.) Also at Haw- 
 ley and at Montague : for a description of which, see the 
 general view of mineral veins and beds that precedes this 
 list of minerals. 
 
 86. Red Oxide of Iron. 
 
 1 . Scaly Red Oxide of Iron. At Kent, Connecticut. 
 
 {Gihbs.) 
 
 2. Red Hematite. At Kent. (Gibbs.) 
 
 87. Brozon Oxide of Iron. 
 
 1. Brown Hematite. At Salisbury and Kent, Connecti- 
 cut. (Silliman.) Also at Westriver mountain in Chester- 
 field, New-Hampshire, in mica slate. 
 
 88. Argillaceous Oxide of Iron. 
 
 1. Granular Argillaceous Oxid of Iron. At Salisbury. 
 (Cleaveland.) 
 
 2. Modular Argillaceous Oxide of Iron. At Putney, Ver- 
 mont, in beds of common clav. The masses are oval and 
 elongated, embracing an earthy nucleus. Also near the 
 falls in Gill, in a dark hard slate of the coal formation. 
 
 3. Bog Ore. At New Braintree, Massachusetts, where 
 it is wrought — also at Greenfield. 
 
 89. Carbonate of Iron, (spathic iron.) At New-Milford, 
 in abundance, {Silliman.) 
 
 90. Sulphate of Iron. Efflorescing on mica slate in small 
 quantities in Conway, Hawley, &:c. 
 
 91. Chromaie of Iron. At New-Haven and Milford ; dis- 
 
 17
 
 120 Geology i ^c. of the Connecticut, 
 
 seminated in the verd Antique marble. {Silliman.) Also at 
 Middlefield in serpentine. {Eaton.) Also at Cummington, 
 well characterized and almost exactly resembling the Bal- 
 timore chromate ; in a loose mass — Found by Dr. J. Por- 
 ter. 
 
 92. Sulphuret of Lead. At Middletown,[Southington, and 
 Huntington, where it is uncommonly argentiferous, and at 
 Bethlehem, (Silliman.) Also at Berlin, (Percival.) Also 
 at Southampton, Montgomery, Hatfield, Leverett, where 
 are two localities, and Whately. At these places the struc- 
 ture of the ore is commonly foliated, sometimes granular 
 and sometimes in cubical crystals. 
 
 93. Carbonate of Lead. This exists in the cavities of the 
 matrix of the lead mine at Southampton. Its colour is 
 white or mixed with yellow. Before the blowpipe it de- 
 crepitated and readily yielded a globule of lead. It occurs 
 crystalized as follows. — 1. Two six sided pyramids united 
 at their bases and deeply truncated at their apices — making 
 fourteen faces to the crystal. — 2. A six sided prism, ter- 
 minated by four sided pyramids, two of the faces being en- 
 larged — fourteen faces to the crystal. — 3* Tabular prisms 
 with bevelments on the edges ; but the precise form I 
 could not determine. These tables frequently cross one 
 another. 
 
 94. Carbonated Muriate of Lead. At the Southampton 
 lead mine in light green groups of cubic crystals, termina- 
 ted by tetraedral pyramids. (Meade.) 
 
 95. Sulphate of Lead. At Huntington with argentifer- 
 ous galena. (Silliman.) Also at Southampton lead mine, 
 in plates or tables on galena. (Meade.) 
 
 96. Phosphate of Lead. At Southampton lead mine, in 
 light green spherical masses, having a radiated structure. 
 
 97. Molybdate of Lead. At Southampton lead mine in 
 tabular, wax yellow crystals. (Meade.) 
 
 98. Sulphuret of Zinc. At Berlin. (Silliman.) Also at 
 Southampton lead mine, foliated and crystallized. The 
 
 «('■.
 
 Geology^ ^c. of the Connecticui. 121 
 
 crystals are so grouped that it is difficult;, in the specimens 
 which I saw, to seize upon the precise fArm. I think, how- 
 ever, I found the octaedron with truncated pyramids. Also 
 at Leverett, foliated. 
 
 99. Arsenical Nickel. At Chatham, associated with ar- 
 senical cobalt. (Pierce and Torrey.) 
 
 100. Arsenical Cobalt! Ai C\idX\idim» (Silliman.) 
 
 • » 
 
 101. Arseniate &f Cobalt. At Chatham. (Pierce and 
 Torrey.) 
 
 102. Oxide of Manganese. At Leverett, in alluvial soil 
 forming; a bed five or six inches thick a (ew inches below 
 the surface. It is in rounded irregular masses from the size 
 of a pea to an inch in diameter and considerably resem- 
 bles granular oxide of Iron. Also at Deerfield ; forming 
 crusts on quartz and mica slate. 
 
 1 03. Native Bismuth. At Huntington. (Silliman.) 
 
 104. Native Antimony. At Harwinton, Litchfield coun- 
 ty, in broad plates. (Silliman.) 
 
 105. Sulphuret of Antimony. At Harwinton.* (Silli- 
 man.) Also near South Hadley. (Gibbs.) 
 
 106. Native Tellurium. At Huntington, associated with 
 tungsten, bismuth, silver, &:c. (Silliman.) 
 
 107. Sulphuret of Molybdena. At Saybrook. (T. D. 
 Porter.) Alsoat East-Haddam and Shutesbury. (Silliman.) 
 Also at Brimfield. (Eaton.) 
 
 108. Yellow Oxide of Tungsten. A new species discov- 
 ered, analyzed and described by Professor Silliman. At 
 Huntington inagangue of quartz. 
 
 109. Calcareous Oxide of Tungsten. At Huntington. 
 (Silliman.) 
 
 110. Ferruginous Oxide of Tungsten. At Huntington. 
 (Silliman.) 
 
 * 104 and 103 need confirmation. — Editor.
 
 122 Geology, ^c. of the Connecticut. 
 
 111. Red Oxideyof Titanium. Near New-Haven — also at 
 Oxford in large gerficulated crystals in mica slate — also at 
 Huntington, at the bismuth, npine ; — crystals as large as 
 the thumb and geniculated. (§i-lliman.) Also at Litchfield, 
 sometimes reticulated on » mica slate. (Brace.) -^Iso at 
 Worthington, Massachusetts, in quartz. (Brace.) -Also 
 at Leyden, in four or eight sides, often- handsomely genic- 
 ulated, generally striated, crystals^in limj)id quartz, tremo- 
 lite and hornblende. Some of the specirbei^ have several 
 geniculations and are as large as the thumb. Hundreds of 
 good specimens have been collected at this locality. Also 
 at Brattleborough, Colrain, Shelburne, and Conway, in 
 quartz, mica slate and tremolite. At Shelburne I found its 
 crystals penetrating a vein of quartz in mica slate in place. 
 In Conway a few small crystals have been observed exhib- 
 iting the primitive form and presenting the "kind of twin 
 crystal," described in Rees Cyclopedia, Art. Rutile. This 
 mineral, indeed, may be found in almost any spot between 
 Conway and Brattleborough, on a strip several miles wide. 
 
 1 12. Silico-Calcareous Oxide of Titanium. At Brattlebo- 
 rough, near the north line of the town in a bowlder of gra- 
 nite, which has flesh coloured feldspar — colour dark brown, 
 or chesnut. Some of the crystals appear to be six sided 
 prisms. (Dewey.) These prisms are terminated, if I 
 mistake not by three sided pyramids. I also noticed a four 
 sided, flattened and striated prism, whose terminations 
 could not be determined. 
 
 113. Ferruginous Oxide of Columhium. At Haddam, in 
 granite. (Berzelius and Torrey.) 
 
 Remark. — Since the above list of localities was comple- 
 ted the following have occurred ; but as they cannot be 
 conveniently inserted in their proper places they may be 
 mentioned here. 
 
 Fibrous Limestone, Satin Spar, in bituminous shale — 
 with Ichthyolites at Sunderland. Andalusite, at Litchfield, 
 Delafield.
 
 GEOLOGY, MINERALOGY, TOPOGRAPHY, &c. 
 
 OF THE CONNECTICUT, 
 
 PART III. 
 
 Scenery. 
 
 BETWEEN the geology and scenery of a country, there 
 is an intimate and interesting connection, l^et the ex- 
 perienced geologist be placed upon an eminence, and the 
 contour of the surrounding region will enable liim to decide 
 with a good degree of probability, concerning the nature of 
 its rocks. The phiin will at once be pronounced alluvion. 
 The swelling hillock or ridge with mural faces — if their 
 aspect be dark — indicate some member of the trap family; 
 if light coloured, they indicate granite. The conical eleva- 
 tion of a reddish hue will be immediately referred to old red 
 sandstone. And those moderately steep hills, that stretch 
 away over many a league, and form continuous and extensive 
 
 * For the map and drawings see V©1. VI. No. I. 
 
 18
 
 124 Geology, S^c, of the Connecticut 
 
 mountain ranges, will be known as mica slate, or gneiss, or 
 some other rock of a schistose structure. 
 
 Such is in fact the aspect of the country along the Con- 
 necticut; and of course we here find a rich diversity of 
 scenery, so that not only the geologist, but the poet and the 
 painter, and every man of correct taste, will find an interest 
 in its beauties. My object at this time is to refer to a few of 
 the most interesting and romantic spots along this river, 
 annexing a short description to each ; in which I shall be 
 most particular concerning those with which I am most fa- 
 miliar. It is not in my power to describe these scenes with 
 the skill of the poet or the painter : But if I can succeed in 
 inducing the traveller to visit them, it will be to him a more 
 agreeable disappointment to have the reality exceed the des- 
 cription, than fall short of it. 
 
 East and West Rock, 
 
 The eminences thus named have long been celebrated, 
 and attract the attention of the visitor who first enters the 
 harbour or the city of New-Haven, as most singular features 
 in the landscape ; — the one lying north west and the other 
 north east, about two miles distant. They present their na- 
 ked fronts towards the city, nearly four hundred feet high, 
 of an iron rust colour ; the original dark brown aspect, be- 
 ing at East Rock principally destroyed by the stone quarry- 
 men, who have, with great boldness, undermined nearly the 
 whole of the front columns for the purposes of architecture. 
 In ascending these cliffs, we find them to be greenstone bas- 
 ed on sandstone.* But when the visitor reaches their top, 
 he will find his attention diverted from the rock on which 
 he stands, to the rich and varied prospect that stretches be- 
 neath his eye. New-Haven, with her long Z/ne of colleges 
 and elegant churches on the one side, and her extensive 
 wharf on the other, is an interesting object ; and suggests 
 to the mind a great variety of agreeable associations. 
 Beyond the city the spectator sees the harbour, grad- 
 ually widening outwards, till it is lost in Long Island 
 Sound ; and low in the horizon, he observes the sandy 
 
 * Cactus opunlia L grows on these rocks as a native.
 
 Geology, ^c. of the Connecticut. 125 
 
 liills of Long Island.* On either side of the harbour the 
 country gently rises into hills of moderate elevation, and 
 is pleasantly diversified with cultivated and uncultivated 
 patches ; and often the neat mansion is seen half covered 
 by the trees. 
 
 East and West Rock become interesting objects to the 
 students of Yale College, being associated with a thousand 
 grateful recollections. To these cliffs they often resort in 
 the hour of relaxation, to enjoy the pleasures of a rich and 
 diversified landscape, to study the geology of the trap 
 rocks and to breathe the serener and more bracing moun- 
 tain air. H ho of them, while standing there, and seeing the 
 white crested waves breaking on the rocky shore, will not 
 remember the ill omened cliffs of Kinsale. 
 
 Prospect Hill, East-Haven. 
 
 Professor Silliman led me to the top of this beautiful 
 greenstone hill, which rises scarcely an hundred feet above 
 the harbour ; but, from its top, the prospect is extremely 
 interesting. New-Haven is presented to you in a direction 
 nearly opposite to that in which it is seen from East or 
 West Rock ; and the view is, in some respects, superior. 
 East and West Rock, seen from this hill, are themselves 
 striking objects in the rear of the city ; constituting the most 
 prominent part of that amphitheatre of hills, which almost 
 encloses New-Haven. Still finther back, mount Carmel 
 and the Berlin moimtains may be seen as you look up the 
 valley of Wallingford River ; and other mountains beyond 
 these till they insensibly mingle with the heavens. Directly 
 in front of the observer, on the west, is iVew-Haven harbour; 
 and a fine opportunity is afforded for witnessing the ar- 
 
 * A few years since, as 1 was crossing the salt marsh at the foot of East 
 Rock, in company with Doct. A. Monson, I observed, on looking towards 
 Long Island, an ancommon instance ol refraction. The shore of that island 
 appeared several degrees higher than usual and uncommonly distinct. In- 
 deed, its altitude seemed as great, as it did a few days previous, when I hap- 
 pened to be sailing within two or three miles of it. It was about noon when 
 this phenomenon was noticed in a clear very hot day of July ; the ther- 
 mometer standing but little below 90°. Did the rapid evaporation produce 
 so great a degree of cold, and consequent condensation of the air near the 
 surface of the water, as to cause this extraordinary refraction .'
 
 126 Geology J ^c. of the Connecticut. 
 
 rival and departure of vessels. Indeed, the beauty of the 
 prospect from this spot is much greater than one would 
 suppose possible from such a mere hillock. The top 
 of the eminence has a circular redoubt upon it, which 
 was constructed by the inhabitants of New-Haven during 
 the Revolutionary war, and repaired during the late 
 war with Great-Britain. The ditch is dug in solid 
 greenstone ; but fortunately not being wanted, it is now 
 abandoned and has become the resort of the flocks that 
 graze in the field ; the magazine serving as a place of shel- 
 ter from the storm.* 
 
 Eminence in West-Haven. — (Now Orange.) 
 
 Near the western line of this town, one or two miles south 
 of the lurnprke from New-Haven to Milford, is an elevated 
 swell of laud, which commands an extensive and delightful 
 pis^ipct. ^Vhen 1 visited il, a thick fog was just breaking 
 a* ay troc. ^developing one object after another, till, at length, 
 the coast af v^'onnecticut from East-Haven to Stratford, and 
 not less than fifty or sixty miles of the coast of Long Island 
 became visible, as well as the villages of Milford andNorth- 
 Milford ; and just rising over the trees, appeared the spires 
 of New-Haven I know not any specific appellation for 
 this commanding plateau. 
 
 Prospect from Middletown, Upper Houses. 
 
 At the north end of the village thus denominated, a few 
 rods from the public house, is a hill, from whose summit 
 is obtained a fine view of the basin in which Middletown is 
 placed, with the city and the river. Here too I had the 
 pleasure, on one occasion, of seeing the various objects of 
 ibis landscape, artificial and natural, partially covered by a 
 foa ; the spires of Middletown and tlie more elevated trees 
 and bills appearine above it, and reminding me of the ante- 
 diluvian world half buried in the deluge. 
 
 * Attached to the red conglomerate at the foot of this hill, I found the 
 beautiful Borrr.ra cJirysophllinlma Ach : And this is the only place in which 
 I have over seen it in New-England, except upon the puddiagstone of Rox- 
 liuf)', Mass.
 
 Geology^ ^c. of the Connecticut, 127 
 
 Monte Video. 
 
 This is a particular part of Talcot Mountain, eight miles 
 northwest of Hariford, at the top of the greenstone ridge ex- 
 tending from Berlin to Amherst. It affords one of the most 
 interesting prospects (and with the exception, perhaps of 
 Hoiyoke, he most interesting) to be found along the Con- 
 necticut. " The diameter of this view, in two directions, 
 is more than ninety miles;'' ad the spires of more than 
 thirty churches are visible, scattered through the broad and 
 delightful vallieson the east and west sides of the eminencct 
 The beauties and subhmities with which nature has invest- 
 ed this sptit, both on a h'mited and an extensive scale, are 
 greatly increased by the displays of an enlightened and cor- 
 rect taste in tile disposition and adaptation of the various ob- 
 jects which this singular country residence exhibits ; such 
 as the tenant's hou.^e in Gothic style ; the summer house ; 
 the boat upon the mountain lake, and rising in Gothic gran- 
 deur above the trees, the hexagonal tower, whose top is 
 nine hundred and sixty feet above the Connecticut. But 
 after the minute and accurate description given by Professor 
 Silliman of these objects and this view, it is altogether un- 
 necessary in this place to go into particulars. To the 
 " Tour between Hartford and Quebec" the reader is with 
 pleasure referred for a complete account of the scenery of 
 Monte Video, which, in some respects, is altogether u- 
 nique in this part of the country. 
 
 Along the same extensive ridge of greenstone, there are, 
 no doubt, many other peaks commanding views of delight- 
 ful landscapes ; but not having visited them, nor seen any 
 account of them, 1 am of course unable to describe them. 
 
 Mount Hoiyoke. 
 
 This is another of the commanding watch towers of the 
 Connecticut. The view from its top is delightful ; and the 
 traveller, whether he be a lover of natural scenery, or a 
 geologist, will find himself amply repaid for turning aside 
 Haifa day to visit its summit. 
 
 Does he look from tfiis elevation with an eye that is ac- 
 customed to range with pleasure over a variegated land-
 
 128 Geology, ^'C. of the Connecticut. 
 
 scape ? Here then wiil he find many forms of beauty and 
 grandeur impressed upon the works of God and man around 
 him. Immediately before him on the west and north, are 
 extensive meadows, through which the Connecticut winds 
 in silence and majesty ; and as if to pay a tribute of respect 
 to this venerable mountain, it here forms a graceful curve of 
 three miles in extent, while its actual advance towards the 
 ocean, scarcely exceeds fifty rods. These meadows are in a 
 high state of cultivation, and during the summer months, the 
 parallel strips, luxuriant with different vegetables, present a 
 charming variety. Just beyond the Connecticut, on the 
 western margin of the meadows, lies the beautiful village 
 of Northampton, vieing for situation and elegance with any 
 country town in New-England. So distinct is the view of 
 this place from Holyoke, that with the naked eye the in- 
 habitants may be seen as they walk the streets ; while their 
 spacious and elegant house of worship, a fine Court 
 House,* and many seats of private gentlemen rise in a rich 
 and diversified relief. A little to the right, in the same 
 valley, the neat villages of Hadley and Hatfield, and still 
 farther to the east, Amherst, with its meeting house and 
 collegiate edifices on a commanding eminence, form resting 
 points in this great basin, on which the eye reposes with 
 pleasure. To the north of these villages the valley of the 
 Connecticut is gradually narrowed by the encroachments of 
 the highlands, until at the distance of about twenty miles, 
 they close in upon it, and beyond this point, a sea of moun- 
 tains displays ridge above ridge and peak above peak, even 
 to the lofty range of the Hoosack and Green Mountains, at 
 the distance of fifty or sixty miles. Southwest appears 
 Mount Tom, a few miles distant, separated from Holyoke 
 by the deep gulf through which the Connecticut flows ; and 
 fifty miles distant, in the northeast, rises the " cloud-capt'' 
 Monadnock. 
 
 Turning southerly, the observer will have a full view of 
 the broad valley extending from Holyoke to Middletown ; 
 a distance of more than fifty miles. He will be able to 
 trace the river, in all its windings, as far as Long Meadow, 
 
 Recently destroyed by fire.
 
 Geology, ^c. of the Connecticut. 129 
 
 which is twenty miles distant; and by an optical deception,* 
 it seems to ascend the whole extent, about as much as it in 
 reality descends; appearing at the farther extremity, to 
 be nearly on a level with the eye. Many pleasant villages 
 are visible along the river ; among which, as most striking, 
 may be named VVindsor, East-Windsor, Springfield, West- 
 Springfield, and South-Hadley and Granby, almost beneath 
 the eye : and these, with th;- many spires of other villageg 
 just visible above the trees, and the alternate patches of cul- 
 tivated and uncultivated ground, checkering the plain, give 
 a liveliness and interest to the commanding landscape. 
 
 I sat down on this eminence, on a clear sumriier day, with 
 a telescope whose power was 40 ; and after the first thrill 
 of adtniration, produced by the general view of the scene 
 around me had subsided, I began to examine, one by one, the 
 objects before me through the glass. The hour divisions 
 and indices, on the dial plate of Northampton meeting 
 house, were as distinct as those on my watch in my hand ; — 
 and I presume an acquaintance might easi'y have been re- 
 cognized in the streets of that place. The divisions, he. 
 on the dial plate of South-Hadley meeting house, five miles 
 distant, were also very distinct. By moving the telescope 
 slowly over the distant landscape, many spires of village 
 churches, that were unnoticed by the naked eye, passed 
 over its field ; and, with little effort, I numbered twenty- 
 four. 
 
 It is a general opinion that East and West Rock are visi- 
 ble from Holyoke. But I am satisfied that the two perpen- 
 dicular bluffs appearing in that direction, are those between 
 Berlin and Meriden ; and that these conceal the New-Ha- 
 ven eminences. On turning the telescope, however, so as 
 to point between the two precipices that are visible, I per- 
 ceived, near the horizon, a low range of hills, about as dis- 
 tinct as the belts of Jupiter; which, I have liule doubt, 
 were a part of Long Island. 
 
 Suppose, next, that the man, who visits Holyoke, is a 
 geologist. He has reached an interesting spot, if he look 
 no farther than the naked trap on which he stands. But he 
 will find his attention, on first visiting this pinnacle, irre- 
 
 • Explained by the rnmmon principles of perspective.
 
 130 *" Geology, f^c. of the Connecticut, 
 
 sistibly drawn to the striking and diversified geological fea- 
 tures beiore him. For he lias a view of nrurly all the sec- 
 ondary region, extending from liew-Haven Hboiit 110 miles 
 northerly j and he sees a vast extent of prim.tive on its 
 borders. As he casts his eye over this extensive tract, he 
 perceives many of those grand chnracteristics ol the differ- 
 ent rock formations, which are not derrved from their com- 
 position, but from a contour, peculiar to c;irh, given by the 
 Almighty Hand that originally produced them : So that if 
 this geologist were unacquainted with the nature of the rocks 
 before him, he would be able to say. with a good degree 
 of confidence ; — yonder hills to the south, so precipitous on 
 the one side, and gradually sloping on the other, must be- 
 long to the trap family. But these extensive unbroken 
 mountain ranges on my right and left, ri>ing so gradually, 
 must be primitive ; and this intervening valley is doubtless 
 alluvion. And on turning his eye northerly, he will pro- 
 nounce the rounded Sugar Loaf and Toby to be sandstone. 
 But it would increase his pleasure, were he to be informed 
 that the former is the Wernerian old red sand.stone, and the 
 latter a peculiar conglomerate of the coal formation, sepa- 
 rated from the red sandstone by a ridge of greenstone ; and 
 that its venerable head overshadows the coarsest granite, 
 and that at its base, pressed down by its enormous weight, 
 may be found cemeteries of fishes that swam in some ante- 
 diluvian stream. He may be pointed also to the South- 
 Hampton vein of lead ore in its whole extent; aud to the 
 localities of the beautiful beryls, sappars, tourmalines, &c. 
 of Haddam and Chesterfield. 
 
 This geologist cannot but perceive that the extensive val- 
 ley, north and west of Holyoke, must, at some remote pe- 
 riod, have been covered by the waters of the Connec'icut, 
 ere the pas -age beiween Holyoke and Tom was worn 
 through — And he will also conclude, that another similar, 
 but much lar2;er lake must have existed in the extensive ba- 
 sin south of Holyoke, before the waters of the Connec'icut 
 had forced a passage through the mountains below Middle- 
 town. Hence he will be led to specidate upon (be pe- 
 riod when these wateis be^an to sub.side and upon the 
 time requisite to wear away such immense masses of rock : 
 and ere he is aware his thoughts will be 1 d back to the 
 period, when the cataract of Niagara began its seven mil«
 
 Geology, fyc. of the Cormecticiit. 131 
 
 retreat, or when the deltas of the Mississippi and Ganges, 
 began to encroach upon the ocean, or even to that time 
 when " all the high hills that were under the whole heaven 
 were covered" with a deluge. 
 
 Last of all, his attention will be directed to the rock on 
 which he stands. And he will find near him those regular 
 columns and those sloping debris, that evince it to belong 
 to the trap family, so singular in its structure and position, 
 and whose origin is so hard to be accounted for.* 
 
 Mount Tom. 
 
 Mount Tom is higher than Holyoke and the prospect 
 from its top is grand and extensive, but there is not that in- 
 teresting grouping of objects in its immediate vicinity ; and 
 while Holyoke attracts so many visitors, Tom is rarely as- 
 cended. Both mountains are merely distinct peaks of the 
 same greenstone range, separated by Connecticut river. 
 
 Sugar Loaf. 
 
 It has already been stated that this is a conical elevation 
 of old red sandstone, rising five hundred feet above the Con- 
 necticut, in Deerfield, immediately on its banks. Any 
 one passing along the stage road from Whately to Deerfield, 
 will be struck with the singular form and aspect of this 
 peak, and be will not regret a visit to its top. This he will 
 find to be an ellipse, whose diameters are about ten and 
 thirty rods. On the east and west sides are perpendicular 
 walls several hundred feet high. Connecticut river is a 
 beautiful object on the east and south, and a bridge across 
 this river, and the village of Sunderland on the opposite 
 bank, appear to be distant scarcely a stone's throw. One 
 fourth of the horizon is hidden on the northeast by the 
 trees. On every other side the view is distinct and com- 
 manding. 
 
 In the meadows near the south point of Sugar Loaf, a 
 skirmish took place in August, 1675, between the Indians 
 and the Massachusetts forces under Captains Lathrop and 
 
 It ought perhaps to be mentioned that recently two commodious build- 
 have been erected upon Holyoke, where the visitor will find ample 
 
 ings 
 
 means of refreshment 
 
 19
 
 132 Geology f ^e. of the Connecticut. 
 
 Beers ; in which the former were defeated with considera- 
 ble loss. And in the plain on the west side of the moun- 
 tain, at a little distance, this same Capt. Lathrnj), in Sep- 
 tember 1675, was drawn into an ambuscade and cut off 
 with his company, consisting of eighty " young men, the 
 very flower of the Coimty of Kssex." Hence the parish of 
 Muddy Brook, which was originally called Bloody Brook, 
 derived its ancient name. 
 
 On Sugar Loaf a two story building has recently been 
 erected for the accommodation of visitors.* 
 
 Mount Toby, 
 
 This eminence is two or three miles northeast of Sugar 
 Loaf, on the east side of Connecticut river in Sunderland. 
 It is made up of the slates and pudding-stones of the coal 
 formation, and is little less than one thousand feet higher 
 than the river, and twice as high as Sugar Loaf. The view 
 from its summit is, of course, more extensive : but as it em- 
 braces for the most part the same regions that are seen from 
 Holyoke and Sugar Loaf, it is unnecessary to be more 
 particular. 
 
 Deerjield Mountain. 
 
 At the highest point of that range of old red sandstone 
 extending from Sugar Loaf to Gill, that is, a little south of 
 the village of Deerfield, on ihe east, is a prospect, which, 
 in one respect, is more perfect than any along the Connec- 
 ticut. It is not very extensive ; but the basin in which 
 Deerfield village stands, presents a picture of rural beauty 
 of singular delicacy and luxuriance. The village, lying at 
 the foot of the mountain and running parallel to it, appears 
 so much beneath the eye, that almost every building in it is 
 dstinclly v.sible. Beyond this, lies one of the richest inter- 
 val tracts to be found in New-England, through which 
 the Deerfield river meanders most beautifully ; and be- 
 yond these meadows, is an amphitheatre of mountains. 
 
 * Growing out of the almost naked rock on the top of the Sugar Loaf, 1 
 noticed the following: rather rare nud interesting: plants : Asclepias verti- 
 cillala. Arttmisia ciiuadcusi , Arbutus uva ursi, Clinipodium vulgare, Poa 
 quinqupfida, Celtis occidentalis, kc. kr.
 
 if 
 
 Geology, c^-c- of the Connecticut. 133 
 
 fVest River Mountain.* 
 
 'J'his is one of those precipitous and partially insulated 
 peaks of mica slate that occur along the Connecticut, and 
 which at a little distance, are often mistaken by the geolo- 
 gist for greenstone hillocks. It is nine hundred and forty 
 feet above the Connecticut, and stands on its eastern bank, 
 directly opposite to the east village of Brattleborough. That 
 village and the intervening river are the most interesting ob- 
 jects in the landscape that is seen from this mountain. One 
 fancies himself almost able, by a single leap from the sum- 
 mit, to throw himself into the village. Almost every other 
 part of the landscape exhibits a tumultuous sea of moun- 
 
 * Tradition has made this mountain volcanic in former days : but obser- 
 vation discovers no traces ol eruption. 'I'he experienced eye of Col. Gibbs 
 (a gentleman who will always be reckoned among the fathers of American 
 mineralogy and geology, first detected t'iie error. (See Bruco's Min. 
 Jour. i\o. 1. p. 19.) While I agree wiih him that the notion of flames said 
 to have been sten issuing IVom ihis mountain .trose " from a popular super- 
 stition through the country, that tlie presence of the precious metals is fre- 
 quently indicated by a flame which arises from the ground at night," I am 
 disposed to adopt the explanation of the accompanying " thunder," given by 
 Dr. Allen ; ("Jour. Sci. Vol. 3 p. 73) who accounts tor this " by the falling 
 ol immense masses of rock." That immense masses of rock have fallen, 
 not only from the cliff* to whi(;h Ur. A. refers, but also from the western 
 face of the mountain, no one will deny who has visited the spot : and that 
 the falling of these would produce a "noise like tliunder," which would be 
 heard two or three miles, no one will doubt who has chanced to be in New- 
 ilaven when the quarrymen had undermined one of the huje columns of 
 Kast Rock aiwl it was precipitated upon the base below. Although two 
 miles distant,^he report in the city is oi'ten as loud as a six pounder. 
 
 In passing over West lliver Mountain a few years since, near the top a 
 rattle snake was announced ; or rather he announced himself by the thrill- 
 ing shake of his rattles. Doct. , (who had been a companion of Wil- 
 son the ornitliologist inone of his pedestrian tonics through the western wil- 
 derness,) immediately despatched the niake and found him to measure a- 
 bove four feet in length. \ mention this fact because it is uncommon in 
 these days in this section of the country to meet with these reptiles. Indeed, 
 1 have never met with another one alive along the (^nnecticut, with per- 
 /(Oyw one exception. I recollect how ver, meeting some years ago a man in 
 Leverett, who was barefoot with several rattle snakes dangling over his 
 shoulders, who told me ho had been hunting them at their den;+ 
 
 * On the fragments of rock at the foot of this cliff, among other interesting 
 lichens grows the Slereocaulon ]iascliale Ach. 
 
 + Rattlesnakes are occasionally killed on all the greenstone ranges of New 
 England, from which they will probably never be entirely extirpated ; a 
 dried one is now before me measuring three feet six inches in length which 
 was killed last summer on the Woodbridge greenstone ridge near New- 
 Haven. — Edilnr, .Mareh 6, '[&2.i.
 
 134 Geology, dj/c. oj the Lotmecticul. • 
 
 tains ; Black mountain on the one hand, and the Monad- 
 nock on the other, beina; prominent, and here and there, a 
 spire, or a village, crowning a hill, or enlivening the val- 
 ley. 
 
 Black Mountain. 
 
 A general description of this mountain has been given in 
 the geological part of this sketch, and I mention it here as 
 presenting an interesting view from its summit. 
 
 Fall Mountain. 
 
 There is a great resemblance between the situation and 
 appearance of this and West River Mountain. Both are of 
 mica slate — both are nearly of the same height — both are 
 precipitous on the west side — both stand on the east bank 
 of the Connecticut — both have a pleasant village opposite to 
 them on the west bank, and both a bridge across the river 
 directly in front. Bellows Falls village is eearer the base of 
 the mountain than Brattleborough, because the river is there 
 narrower. The observer from the top of Fall Mountain 
 looks down almost perpendicularly upon the Connecticut, 
 here reduced to a few rods in width, and foaming and falling 
 among the jutting rocks, presenting an image of disorder 
 and danger, while the neat village on the river's bank exhib- 
 its an image of peace and security. 
 
 Nutnerous other eminences in the primitive mountain ran- 
 ges on either side of the Connecticut, commana extensive 
 and interesting prospects. But the most conspicuous have 
 been described, it is unnecessary to go into farther particu- 
 lars. 
 
 Bellows Falls. 
 
 Every thing at this romantic spot conspires to impress 
 the beholder with the idea of wild sublimity. The perpen- 
 dicular fall ol the water is of no great height ; but the whole 
 stream is here compressed into a channel of a few rods in 
 width, worn out of solid granite, a quarter of a mile, or 
 more, in length, down which the current dashes, as if impa- 
 tient of its confinement in so narrow a bed : and at the foot 
 
 c
 
 Geology^ ^c of the Connecticut. 135 
 
 of the sluice, it spreads out again into its accustomed width 
 and soon resumes its wonted calmness. 
 
 Near the middle of these Falls a bridge is thrown across 
 the river, and from this, a fine view is afforded of the ra- 
 pids and surrounding scenery. The first time 1 visited the 
 spot, I chanced to cross this bridge from the east, as the 
 evening twilight was dying away, and there was just indis- 
 tinctness enough upon objects to leave room for the play of 
 the imagination. In the middle of the bridge I stopped and 
 looked into the foaming stream below, where the ragged 
 rocks, half seen amid the partial darkness, jutting out from 
 the banks and shooting up from the bottom, presented a 
 real Charybdis, devouring whatever entered its jaws. Dan- 
 gers enough were visible, in the dark waters below ; and 
 while nothing but the bridge seemed to separate me from 
 destruction, on looking up, I saw the venerable Fall moun- 
 tain, rising with its impending precipices, and threatening 
 to bury the whole in ruins. 
 
 Nearl)- a mile below the falls, on the Vermont side, is a 
 favourable spot for viewing them and the surrounding 
 scenery. From this point you see the cataract nearly in 
 front, with the bridge crossing it at right angles, with the 
 line of vision ; while the mountain, here seen in its whole 
 length, forms a lofty mural barrier on the eastern bank. At 
 the foot of this mountain, just beyond the bridge and al- 
 most overshadowed by the shaggy rocks, stands a large and 
 elegant mansion house ; and on the opposite side appears a 
 neat compact village. 
 
 Turner^ Falls. 
 
 These cross the Connecticut, near the point where the 
 (owns of Greenfield, Gill and Montague meet. There is no 
 distinctive name by which they are known in the vicinity j* 
 
 * Professor Silliman denominates this cataract iMiller's Falls (See Tour. 
 to Quebec, p. 400.) But Millers Falls are three miles higher up the riv- 
 er, at the mouth of Miller's river, and not in the Couuecticut. 
 
 A few years since an Indian, who lived near Turner's falls, was precipi- 
 tated over them : But by his dexterity in swimming;, and by placing his 
 feet forward as he descended, he escaped alive. Some time afterward, 
 however, as the ice in the spring time was breaking up, he was unfortu- 
 nately carried over aniong the broken fragments and never appeared again.
 
 136 Geology^ fyc. of the Connecticut. 
 
 and I have ventured to denominate them Turner's Falls, for 
 a reason that will appear in the course of the description. 
 
 The river at this place runs in a northwest direction, 
 crossing the rock strata nearly at right angles ; and an arti- 
 ficial dam is raised upon these rocks of the coal formation, 
 so that the whole stream, which is here more than one 
 thousand feet wide, falls thirty feet perpendicularly. This 
 sheet of water, however, is divided near the middle by a 
 small island on which the dam reposes. For three miles 
 below the principal descent, the water continues to descend 
 so as to render a canal necessary. 
 
 The proper and almost the only spot for viewing this 
 cataract to advantage is on the elevated ground forty or fifty 
 rods below the falls on the northeast shore.* Standing on 
 this spot, you have the principal fall of water nearly in 
 front, or at right angles with the line of sight ; and you can 
 see the river above and below the dam one or two miles. 
 The contrast, is, however, very great. Above the cataract the 
 water is unruffled to the very verge of the precipice, down 
 which it rolls in graceful majesty. Below, it tumbles and foams 
 among the rocks as far as the eye can trace it. A little far- 
 ther down the stream than the station of the observer, the 
 river strikes directly against a greenstone ridge,f two hun- 
 dred feet high, by which it is forced to curve to the left, 
 more than a quadrant, and afterwards runs nearly south. 
 The rocky island that divides the cataract, with the white 
 foam dashing against the base of its cliffs and its top crown- 
 ed with a few pines and other shrubbery, is a picturesque 
 addition to ihe scenery. Several rods below this island a- 
 nother is planted of similar aspect, but smaller, and at a 
 much lower level, and apparently inaccessible. The upper 
 island may be reached by a canoe in safety ; and then we 
 can descend to the very foot of the falls and find the voice 
 drowned by their roar; and in favourable circumstances, 
 see the rainbow arching over the falling sheet. 
 
 * From this spot a view of these falls was taken, in 1818, by a friend, and 
 inserted in the Port Folio for December of that year, with a short descrip- 
 tion. The dam has recently been removed several rods down the stream ; 
 so that the present, view differs a little from the drawing which was theu 
 executed ; and the removal of the dam, I think, has ra'.her injured the view. 
 
 + At the foot of this ridge, in the bottom ol^ the stream, and adhering to 
 the rocks, grows in abundance the singular Lemaniajluviatilis of Agardh.
 
 Geology, ^'C> of the Connecticut. 137 
 
 The country around these falls is little cultivated and there 
 are but few settlements on either side of the river. In al- 
 most every direction you see gently rising hills, covered 
 with trees; of which the pine forms a large proportion. For 
 three miles above the falls is a fine spot for a sailing excur- 
 sion. You immediately enter between wooded, and mode- 
 rately elevated hills, exhibiting all their original wildness ; 
 and so placid is the stream, gently curving among these hills, 
 now and then spreading out so as to form coves along the 
 shore, and here and there chequered by small islands, that 
 you fancy yourself to be in the midst of a romantic moun- 
 tain lake. To the coves along the shore, parties frequent- 
 ly resort for taking fish. 
 
 These and other circumstances render Turner's falls and 
 the vicinity an attractive spot to any one who takes an in- 
 terest in the wild and sublime scenes of nature. By a refe- 
 rence to the preceding part of this sketch, it will be seen 
 that the geologist and mineralogist will find here much to 
 awaken and gratify curiosity.* 
 
 Bellows and Turner's falls are in many respects very dis- 
 similar. At the former, the river is narrow and the fall, 
 viewed by itself, is not the principal object of interest ; but 
 at the latter, the Connecticut pours a broad and unbroken 
 sheet of water over a precipice comparatively lofty, produ- 
 cing a roar that is frequently heard at the distance of twelve 
 miles. 
 
 One hundred and fifty six years ago, a party of Philip's 
 Indians, having joined those residing in Platfield, Deerfield, 
 &tc. all being at war with the white inhabitants, resorted to 
 Turner's falls to take fish, and encamped on the north east 
 shore. On the 1 7th of May, Capt. Turner from Boston, 
 marched from Hatfield with one hundred and fifty men, 
 consisting of the garrison and militia from Springfield, 
 Northampton and Hatfield, and came by surprize upon the 
 Indian camp the next morning at day light. The Indians 
 were totally unprepared for the attack, and fled in every di- 
 rection. Some sprang into their canoes, and pushing from 
 the shore without paddles, were hurried over the cataract 
 
 * I am at a loss to account for it, that t'lese falls have exciteJ so little at- 
 tention and drawn so few visitor?. They are but three miles from the vil- 
 lage of Greenfield, the road is gf»d, and the accommodations decent, at a 
 public house on the bank.
 
 133 Geology, ^-c. of the Connecticut. 
 
 and dashed in pieces — while some reached the opposite 
 bank. Three hundred lodians are said to have been killed 
 and only one Englisliman. Yet the Indians who survived, 
 being joined by another party, fell upon the English troops 
 as they were returning and made dreadful slaughter among 
 them. So that before they reached Hatfield, Capt. Turner 
 was killed, and thirty seven of his men. 
 
 After reading this piece of history, no one will doubt the 
 propriety of denominating this cataract Turner's Falls. 
 
 Shelburne Falls. 
 
 These are in Deerfield River in the west part of Shel- 
 burne : and a partial description has already been given of 
 them in this sketch. I know of nothing concerning these 
 rapids that requires particular description. Visiting them at 
 low water, however, I was much struck with the number 
 and magnitude of those spheroidal excavations in the rock 
 called pot holes. They are often seen several feet in di- 
 ameter and depth, and the stones, <Sz;c. by which the water 
 wears them out, are still found at their bottom. 
 
 PART IV. 
 
 Miscellanies. 
 
 The greater part of the subjects to be jjresented under 
 this division might, without impropriety, have been connect- 
 ed with the first, or geological part. But as that division 
 had swelled more than was expected, it was though! best 
 to throw them together at the close of the Sketch. Some 
 of the following articles however have suggested themselves 
 since the geological part was written. 
 
 Ancient Lakes. 
 
 Any one who examines the passage of the Connecticut 
 and many of its tributaries, through several mountains em- 
 braced by the Map accompanying this Sketch, will be led, 
 I think, to the conclusion that the waters of this river once 
 flowed over the great valley along its banks, forming an ex-
 
 Geology, ^c. of the Conneclicut. 139 
 
 tensive lake : and also, that when this began to subside, by 
 the wearing away of the outer barriers, other barriers would 
 appear and produce other lakes of inferior extent. 
 
 It is no argument, as some have thought, in favour of 
 such a supposition, that so much rock occurs in this basin 
 which is evidently a recomposition of the detritus of 
 older formations ; and that organic remains are found 
 in these rocks. For every geologist knows that all this 
 must be referred to a period anterior to that, in which 
 the last grand diluvian catastrophe happened to the 
 globe and left our continents in their present form.* Nor 
 is the mere occurrence of masses of stone, evidently round- 
 ed by the attrition of running water, any evidence in favour 
 of this hypothesis ; for we must look for the cause of this 
 also, as far back at least as the Noachic deluge. — No cur- 
 rent of water with which we are acquainted is sufficient to 
 transport such masses of rock into the situations in which 
 we find them : " for though we can readily conceive how the 
 agency of violent currents may have driven these blocks 
 down an inclined plane, or, if ihevis a lergo were sufficient, 
 along a level surface, or even up a very slight and gradual 
 acclivity, it is impossible to ascribe to them the Sisyphean 
 labour of rolling rocky masses, sometimes of many tons in 
 weight, up the face of abrupt and high escarpments."f 
 Rounded masses of rock may however occur under such 
 circumstances as to show them to have been removed by 
 currents posterior to the deluge. 
 
 The principal evidence in favour of the supposition that 
 the waters of the Connecticut once flowed over the broad 
 valley on its banks, consists in the appearance of the chan- 
 nel of the river where it passes through certain mountains. 
 Thus, every one perceives that this river must have cut its 
 deep passage through the mountains below IVliddletown : 
 in other words, this supposition will account for that gulf 
 several hundred feet deep in which this river now flows, and 
 we are not acquainted with any other agency that will ac- 
 count for it. And if it be admitted that this passage was 
 
 * See some excellent remarks on this subject in the recent work of Cony- 
 t>eare and Philips, entitled " Outlines of the Geology of England a£d 
 Wales"— page 57 Introduction. 
 
 t Vid. same work page 29, Introduction. 
 
 20
 
 140 Geology, ^c. of the Connecticut. 
 
 once closed up nearly to the general level of the neighbour- 
 ing mountains, it must have thrown back the waters of the 
 Connecticut over the whole of the secondary tract marked 
 on the map, with the exception of some of the highest 
 ridges and peaks of greenstone and sandstone, which then 
 probably formed islands in this extensive expanse of wa- 
 ters. 
 
 At the outlet of the Connecticut through the mountains 
 below Middletown, a little south of the Chatham cobalt 
 mine, and six or seven hundred feet above the present bed 
 of the river, I saw rounded masses of old red sandstone, 
 several inches in diameter, mixed with the fragments of the 
 rocks in place. Such a fact I never noticed at any other 
 place in the primitive region along the river : certainly not 
 on the east side of it. And I was led irresistibly to the con- 
 clusion, that they were conveyed thither by the ice of the 
 ancient lake, which would be floated to the ocean through 
 this outlet. 
 
 In the northern part of the tract supposed to have beeo 
 covered by this lake, other evidences of its existence pre- 
 sent themselves. In the southern part of Deerfield, the 
 sandstone cliffs of Sugar Loaf, four hundred feet above 
 the present level of the Connecticut, bear evident marks of 
 having been worn and undermined by water : — that is, they 
 appear very much like similar rocks which now form the 
 beds and banks of the Deerfield and Connecticut rivers. In 
 the north part of Deerfii^ld, at the west foot of the green- 
 stone ridge, and two hundred feet at least above the Con- 
 necticut, is the channel of a stream ten or twelve rods wide, 
 that once ran southerly, as appears from the little eminences 
 of greenstone that were exposed to its action, which pre- 
 sent a perpendicular front on the north side, while the south 
 side is sloping and pres^ents an accumulation of brokea 
 pieces of the rock. One mile west from this spot, and a 
 few rods south of the village of Greenfield, appears the 
 bed of a smaller stream which there formed a cataract,* of a 
 few feet over a ledge of red sandstone rocks. In this rock 
 are numerous spheroidal excavations of two or three feet in 
 depth, leaving no doubt that a current of water once flow- 
 ed there. This channel is less than one hundred feet above 
 
 * See Dickinson's View of Massachusetts, p. 33.
 
 Geology, ^c. of the Connecticut. 141 
 
 the Counecticut. A little to the northeast and especially 
 one or two miles northwest of the village of Greenfield, the 
 old red sandstone rocks are smoothed and fluted in a great 
 many instances; indicating a former exposure to currents 
 of water. These various circumstances render it very 
 probable that the country was once covered by a lake. 
 
 As the passage of the Connecticut through the moun- 
 tains below Middletown was gradually worn deeper and 
 deeper, this lake would be lowered also — and in process of 
 time, the lofty greenstone ridge, extending from near New- 
 Haven to Amherst, would present another barrier, and at 
 length the original lake would be divided into two ; the one 
 extending from Northfield, on the west side of this ridge, 
 nearly to New-Haven, and the other, on the east side, from 
 South-Hadley to Middletown. There is every appearance 
 that the Connecticut has worn down a passage through this 
 ridge between Holyoke and Tom. 
 
 As this process of draining continued from century to cen- 
 tury, these lakes constantly contracted their limits, until at 
 length the greater part of the extensive vallies they occu- 
 pied were laid bare. In the western lake however, were 
 three basins, at Farmington, Westfield and Deerfield, a few 
 miles in extent, which would remain filled with water until 
 the three rivers of the same name, which supplied them, 
 had worn away passages through the greenstone ridge above 
 mentioned. That they have done this, will be doubted by 
 no one who will examine their course through this mountain. 
 
 Thus after the lapse of years would these lakes all be 
 drained, leaving a rich valley for cultivation. And whoev- 
 er will examine the alluvium of Farmington, Westfield and 
 Deerfield, will be led to suppose that the period when the 
 work was finished could not have been many centuries ber 
 fore the settlement of this country. 
 
 Sunderland Cave. 
 
 This is about three miles northeast of the village in the 
 rocks of the coal formation. It forms nearly a quarter of a 
 circle, is about ten rods through, opens on the north and 
 west, is from two to twenty feet wide, and from ten to sixty 
 or seventy deep. A few rods to the south is a fissure ten 
 feet wide, nearly parallel to the cave, and sixty or seventy
 
 14:2 Geology, i^'c. of the Conncclicut. 
 
 feet deep. Both the cave and tb.e fissure are in an immense 
 mass of pudding stone with scarcely any thing hke stratifica- 
 tion ihroughoui ; and this is incumbent upon a soft, decom- 
 posable, argillaceous sandstone slate. The disintegration 
 of this slate, either by the waters of the lake above des- 
 cribed, or by simple exposure to the vicissitudes of the cli- 
 mate, has probably caused tliis enormous stratum of con- 
 glomerate to fall partially down and thus to form the cave 
 and the fissure. 
 
 favourable situation of Yale College as a School of Aline' 
 ralogy and Geology. 
 
 It is a curious circumstance, that this Institution should 
 have been fixed by its founders, who must have been alto- 
 gether unacquainted with geology, at the very focus of 
 most of the Wernerian rock formations. It stands at the 
 southern extremity of the secondary region of the Connec- 
 ticut; and had experienced geologists searched the whole 
 of New-England, they could not have found a more eligible 
 situation for a geological and mineralogical school. It is 
 also a fortunate coincidence of favourable accidents, that 
 the first mineral cabinet in the United States should have 
 been deposited in Yale College, before there was much 
 known concerning the interesting nature of the surrounding 
 country. 
 
 The geological professor at Yale could, even from his 
 lecture room,* point out most of ihe rock formations of the 
 globe. He could direct the attention of his pupils to the 
 plain around them, as alluvium ; and to the hills of Wood- 
 bridge and Milford, as exhibiting interesting deposites of 
 diluvium. On the north they would see the striking sec- 
 ondary greenstone eminences of East and West Rock ; and 
 on the west, hills of primitive greenstone. In this same di- 
 rection, only four or five miles distant, he might point them 
 to the West-H:iven chlorite slate, to the Woodbridge argil- 
 lite, to the iMilford verd antique and serpentine, and a little 
 beyond, to the mica slate. A few rods to the north, or 
 east, they might see the old red sandstone and the green- 
 
 , •' The cabinet which is in the third story of ;\ his^h building and in which 
 the lectures are given commands a view ol'the noi^hl-ourii'ig hills.
 
 Geology, fyc. of the Connecticul. 143 
 
 blone dikes they contain. In East-Haven, also, six miles 
 distant, occur the red and grey slates of the Coal Forma- 
 tion ; in Northford, the fetid carbonate of lime ; at South- 
 ington the bituminous limestone ; at VVestfield the bitumin- 
 ous shale with ichthyolites ; at Durham the coarse con- 
 glomerate of the coal formation, and at Berlin the green- 
 stone and slates of the coal formation with interesting locali- 
 ties of coal, galena, blende, barytes, agates and zeolites in 
 the greenstone — all within lialf a day's ride. In East-Haven 
 appears the sea beaten granite ; and, a little farther to the 
 north and east, the gneiss, hornblende slate and mica slate 
 formations. 
 
 The mineralogy of the vicinity of Yale, is also rich and 
 diversified. Suffice it just to mention the chalcedony, car- 
 nelian, amethyst, agates, stilbite, zeolite, laumonite, preh- 
 nile, analcime, &ic. of the neighbouring greenstone : the na- 
 tive copper, copper and lead ores, so abundant in the same 
 formation : — the native silver, bismuth, magnetical and com- 
 mon pyrites, galena, blende, the three ores of tungsten, the 
 tellurium, fluor spar, epidote. titanium, he. of Huntington : 
 the asbestus, bitter spar, sahlite. serpentine, &;c. ofMilford : 
 the cobalt ores at Chatham ; the corundum, andalusite,* 
 &ic. of Litchfield ; and the chrysoberyl, beryl, tourmalines, 
 garnets, magnetic iron, columbium, he. of Haddam. 
 
 Geological Position of Amherst Collegiate Institution. 
 
 This is situated on elevated ground, and commands an 
 extensive and delightful view af the surrounding country. 
 It stands on granite, here covered by diluvium ; but the 
 granite appears a short distance both north and south. On 
 the west, stretches out an alluvial plain ; on the south, rises 
 the lofty Holyoke of greenstone ; on the east, of gradual as- 
 cent, a mUl^foif of gneiss ; on the north, appears, a few 
 miles distant, mount Toby, composed of rocks of the coal 
 formation ; and also the rounded Sugar Loaf of old red 
 sandstone : — while beyond the alluvial tract, on the west, 
 rises a high range of mountains made up of granite and sie- 
 nitic granite, (containing the interesting lead mine of South- 
 
 '''■ RecenUv announced by Maior Delafipld. Vide Anaer. Journ. Sci. Vol. 
 6. p. 176.
 
 144 Geolvgi/, ^c. of the Connecticut' 
 
 Hampton,) primitive greenstone, greenstone slate, mica 
 slate and gneiss, so that without mentioning the rare mine- 
 rals found in the vicinity, it is evident that an interesting 
 assemblage of rocks is presented in the neighbourhood fof 
 the instruction of the geological student. 
 
 Fac Simile of Goshen Graphic Granite. [See Plate I, Fig. 1.] 
 
 A description of this granite has been already given in the 
 First Part of this Sketch. But having since discovered 
 some more perfect specimens, I thought it might not be un- 
 acceptable to have one of them copied. It is not common 
 to find specimens so well marked as the one from which the 
 plate was taken ; yet, in general, they are quite handsome. 
 The points, triangles, &;c. of quartz, usually enlarge, or di- 
 minish, as they traverse the feldspar. Thus, the specimen, 
 of which the plate is a copy, exhibited on its opposite side 
 (about four inches distant from the surface that was copied,) 
 the same characters but four times as large. 
 
 Pseudomorphous Granite. [See Plate 1, Fig. 2.] 
 
 It is not an easy matter to give a good graphic represen- 
 tation of this rock. Perhaps however, the one annexed may 
 assist in understanding the description given on p. 17, ^riSp** 
 The dark part represents the plates of mica ; — the red part 
 the quartz, and the uncoloured portion, the feld'^par. This 
 rock occurs abundantly in Goshen, connected with the 
 graphic granite above described ; and the transition of the 
 one into the other is usually very sudden. 
 
 Lusiis Naturae. [See Plate I, Fig. 3.] 
 
 For a description of this, see page 15, 
 
 Desiderata in the Geology and Mineralogy of the Connec- 
 ticut. 
 
 It may be remarked in general, that but a small part of 
 the geolog} and mineralogy of this region has been brought 
 to that degree of perfection to which these sciences have 
 been carried in some countries in Europe ; and, therefore,
 
 Geology, ^c. of the Connecticut. 145 
 
 there are desiderata in the whole. But some parts are more 
 deficient than others ; and I shall take the liberty of noting 
 some of those points which seem more particularly to de- 
 mand the further attention of the geologist. Among these 
 the following may be named. 
 
 1. A more exact determination, in many instances, of 
 the boundaries of the several formations. 
 
 2. Further examination of the exact relative position of 
 the old red sandstone and the coal formation. 
 
 3. Further search for greenstone dikes, not only in the 
 old red sandstone, but also in the coal formation, and even 
 in primitive rocks. 
 
 4. Whether the beds of secondary greenstone detach 
 veins from one to the other, as in the isle of Sky. 
 
 5. A further examination of the granitic beds, to deter- 
 mine whether like connecting dikes or veins may not be 
 found uniting them also. 
 
 G. A more thorough search to ascertain whether all our 
 granite does not exist in the form of beds and veins. 
 
 7. To find more instances in which the coal formation and 
 greenstone form alternating beds. 
 
 8. An examination of the beds of clay and gravel, found 
 along the Connecticut, for shells and other organic remains. 
 
 9. Further search in the coal formation for organic re- 
 mains.* 
 
 10. Examination of the bituminous limestone of South- 
 ington, especially with the query of Prof. Silliman in mind, 
 (Journal p. 63, vol. 6.) whether this rock may not itself be, 
 or be connected with, bituminous marl slate .'' 
 
 11. The extensive range of greenstone, running from Ber- 
 lin to Amherst has as yet been but little examined for mine- 
 rals, as well as many other greenstone ridges. Indeed, the 
 mineralogy of this whole region requires farther explora- 
 tion, and promises the diligent student much fruit. 
 
 Meteorological Fact. 
 
 The following circumstance, although connected with 
 geology, does not strictly come within the limits of this 
 
 * Dr. Cooley informs me that he has recently discovered another locali- 
 ty of ichthyolites in Deerfield, about three milts from the locality in Snn 
 cterland.
 
 146 Geology y ifc. of the Connecticut 
 
 Sketch : Yet it seems worth noticing, but hardly of suffi- 
 cient importance to form a separate paper. 
 
 In goinii westward from Connecticut river, we first pass 
 over an alluvial tract and then continue gradually to ascend, 
 for twenty miles, to the top of Green and Hoosak moun- 
 tains. As might be expected, the winters on this elevated 
 land continue two or three weeks later than in the valley ; 
 that is, the farmer can sow his seeds two or three weeks 
 earlier in the valley than on the hills. But in autumn, 
 the destructive frosts are usually as much later on the hills 
 than along the river : — so that one frequently passes from 
 the river in October, where almost every vegetable is des- 
 troyed, and finds the crops uninjured on these bills ; and 
 the crops there are about a fortnight later than those in the 
 vallies, so as to require this lengthening out of their time of 
 ripening. I have been disposed to attribute this fact to the 
 greater moisture of the atmosphere of the vallies, arising 
 from the more copious exhalations from the river, whereby 
 the efFec<s of frost are greatly increased, even at the same 
 temperature. 
 
 Tabular Arrangement of the Rock Formations alonz, the 
 Connecticut* 
 
 * I here follow with pleasure the very simple yet ingenious arrange- 
 ment of rocks, which is adopted by Conybeare and I'hillips, as the basis 
 of their recent work on the Geology of England and Wales. It has the 
 rare merit of being entirely free from hypothesis. It would be well if a 
 similar purification from the alloy of uncertain systems, could be extended 
 through every part of geology. The work, however, is rapidly advancing 
 and in the hands of such men as the authors of this work, and of McCul- 
 loch, Greenough, Buckland, Webster, Borre, Cuvier, Brongniart, Uc. we 
 confidently expect that it will be speedily accomplished. 
 
 In the above tabic, I may have put down some rocks in the Inferior Or- 
 der, which the authors of this arrangement will place in the Submedial Or- 
 der. For tlieir acooimt of these orders is not yet published ; and in the 
 general sketch, they have given, only a part of the rocks belonging to each 
 . inter are enumerated.
 
 Geology, fyc. of the Connecikvt. I4T 
 
 I. Inferior Order. 
 
 ^Common 
 Gra- Porphyritic 
 Dite.< Graphic 
 Pseudo- 
 morphous 
 
 (No. 
 
 2. Sienite, or Sien- 
 itic Granite' 
 
 3. Gneiss. 
 
 Com- 
 
 mou i 
 Glandii- I 
 [_ Iqus 
 
 Rocks observed in contact icith 
 thoie in lite leading column. 
 ^Sienitic Granite ^ N. Hampton, Belchert'u,ic, 
 " I Leveretl granitic range, 
 
 I Do. Gr^.riville, (fee. 
 I Conway, VVilliamsburgh,^C; 
 j- V\ estfield, Mass. 
 
 Conway 
 
 Passim 
 Northampton 
 
 1 Northampton, &C; 
 Chatham. 
 VWhately. 
 I Do. 
 
 J Northampton. 
 ^ Leverett, ice. 
 I Passim. 
 
 4. Hornblende 
 
 Slate 
 
 5. Mica Slate 
 
 L 
 
 6. Talcous Slate 
 7. 
 
 Gneiss 
 
 Hornblende Slate 
 Mica Slate 
 Serpentine 
 Limestone, 
 
 7.) 
 Diluvium 
 Alluvium 
 Granite 
 
 Hornblende Slate 
 Primitive Greenstone 
 Diluvium 
 Alluvium 
 'Granite 
 
 Hornblende Slate 
 
 White (iran. Limestone ! Litchfield County. 
 Mica Slate [Leveiett, Granville, 
 
 Steatite | New-Salem. [S;c. 
 
 Diluvium J Passim. 
 
 ^Granite "^ Granville, k.a. 
 
 Sienitic Granite | Ch.aham. 
 Gneiss }• Passim 
 
 I Mica Slate I Shelburne, Colerain, &c. 
 
 I Diluvium J Passim. 
 
 ^'Granite "1 Conway, &c. 
 
 Gneiss I Monson, Wilbraham, v<:c 
 
 Hornblende Slate | Shelburne, Heath, kc. 
 Limestone, (No. 7) | IJeerfiekl, Conway, &c. 
 Argillile I Leyden, VVoodbridge, &c. 
 
 Chlorite Slate | VVhitingham, Milford 
 
 Greenstone Slate ^VVhately, Do. 
 
 Serpentine .Middlelield. 
 
 Steatite New-Fane, &c. 
 
 Old Red Sandstone Passim. 
 Coal Formation S. Hampton Lead Mine. 
 
 Diluviuai Passim 
 
 vuini 
 
 l^Alhi 
 
 ^ Mica Slate 
 
 I Chlorite Slate 
 
 J Wilbraham. 
 
 Plaiufield, Hawley, &c, 
 Whitinsham. 
 
 Limestone, or a Granitic i Granite (in veins) 1 Conway. 
 A;;gregateof Silex, Carb. ? Mica Slate > Deerfield, 
 
 ' " ( .Argillite ) Putney. 
 
 &c. 
 
 Lime and Mica 
 
 ■^ This is undoubtedly (he rock denominated sienitic granite, by Dr. Mc 
 Culloch, in his Geology of Glen Tilt. (Geo!. Trans. Vol 3. p. 299 and 300.) 
 That is, he regards it as a mere variety of granite, distinguished from other 
 varieties by the presence of hornblende in any proportion. Had I read his 
 memoir on the Tilt belbre the geological part of this sketch was written, I 
 should not have separated sienite from granite, but have treated the two 
 rocks as mere varieties. 
 
 21
 
 148 
 
 Geology, ifc. of the Connecticut. 
 
 8. Chlorite Slate 
 
 9. Steatite 
 
 10. Serpentine 
 
 Rocks observed in contact with those in the. leading column. 
 
 Talcous Slate ^ Whiting ham. 
 Mica Slate I Do. 
 
 Argillite | Guilford, Vt. and Woodbridge. 
 
 Verd Antique J-Milford. 
 
 Prini. Gre«ustone Do. 
 Diluvium Do. 
 
 Alluvium j Orange, (Ct.) 
 
 Gneiss ) New-Salem. 
 
 Mica Slate \ Middlefield. 
 Serpentine ) Do. 
 
 Granite "j Westfield, Mass. (Eaton.) 
 
 Mica Slate [Middlefield, (Dewey.) 
 
 Granular Limestone f Milford. 
 (_ Steatite J Middlefield, 
 
 n ir -^ A 1- ^ Primitive Greenstone ? Milford. 
 
 11. Verd Antique J C^j^^j^^gl^^^ 1 Do. 
 
 f Mica Slate 
 I Chlorite Slate 
 
 12. Primitive ( Unstratified j Sienite 
 
 Greenstone I Greenstone Slate ] Verd Antique 
 
 I Old Red Sandstone j Whately, Gill. 
 LCoal Formation J Gill,Northfield. 
 
 The order of succession of the seven preceding rocks is very variable and 
 uncertain. 
 
 (Do.) 
 
 ^ Wolcott ? 
 I Milford. 
 [Whately. 
 f Milford. 
 
 II. SuBMEDiAL Order. 
 
 13. Argillite 
 
 rMica Slate 
 Limestone, (No. 7.) 
 Prim. Greenstone 
 Chlorite Slate 
 Old Red Sandstone 
 Diluvium 
 Alluvium 
 
 Putney, Woodbridge. 
 
 Do. 
 
 Woodbridge. 
 
 Do. 
 
 Do. 
 
 Do. 
 
 J Brattleborough. 
 
 III. Medial Order. 
 
 14. Old Red ) Common > 
 
 Sandstone ^ Conglomerated ^ 
 
 fGranite 
 
 Mica Slate 
 I Argillite 
 
 J Prim. Greenstone 
 j Second. Greenstone 
 I Coal Formation 
 I Diluvium 
 [^Alluvium 
 
 Northampton. 
 Deerfield.
 
 Geology, <^*c. of the Connecticut. 
 
 149 
 
 2- ^ 
 
 u 
 
 to ;3 
 
 Very Micaceous 
 Black tortuous 
 Bituminous Shale 
 Finer Puddingstone 
 Coarse Do. 
 
 r 
 
 I Compact 
 J Columnar 
 I AmygJaloidal 
 I Porphyritic 
 
 L 
 
 Rocks observed in contact ivilh 
 those ill the leading column. 
 
 Wacke* 
 
 Trap Tuff 
 
 Dark bastard Limestone 
 
 Bituminous Do. 
 
 Fetid Do. 
 
 Seams of Coal 
 
 Fine red arg;. Sandstone 
 
 Coarse gray Siliceous Do. 
 
 Do. 
 Do. 
 
 J 
 
 fGranite 
 
 I Gneiss 
 Mica Slate 
 (Old RedSandstone 
 Prim. Greenstone 
 Sec. Greenstone 
 Diluvium 
 |_Alluvium 
 
 Southampton f 
 
 Montague. 
 
 S. H.leadm. 
 .Passim. 
 ''Gill. 
 
 Passim. 
 Do. 
 
 Enfield, (Ct.) 
 
 Granite ") East-Haven i* 
 
 Old Red Sandstone I East and West 
 
 ^ Rock. 
 Coal Formation ! Gill, Berlin, Sic. 
 
 J 
 
 IV. Superior Order. 
 
 17. Diluvium 
 
 18. Alluvium, 
 
 Above most or all of the preceding ibrmations. 
 Oceanic deposites "] 
 
 Beds of Gravel j 
 
 Do. Clay \ Above most of the 
 
 Clay 
 Sand 
 
 Do. 
 \ Loam 
 [_Decom posed Rocks and Vegetables_ 
 
 (preceding formations. 
 
 * Prof. Silliman has decided, in the affirmative, the question wheth- 
 er this rock exists along the Connecticut. Vide Journal of Science, Vol. 
 6. p. 51 note. 
 
 t In Conybeare and Phillips' late interesting work on the Geology of 
 England and Wales, (p. 311,) the Bituminous Marie Slate, with the ac- 
 companying limestones, sandstones and conglomerates, is placed in the su- 
 permedial order ; that is, immediately above the rocks of the coal Forma- 
 tion ; and if the Rocks above denominated the Coal yormatiou should 
 prove to belong to the Bituminous Marlite Formation, according to Mr. 
 Brongniart's opinions, they must be placed in the ?upermedial order also. 
 But what becomes of the old red sandstone (rothe todte liegende) which lies 
 immediately below the Bituminous Marl Formation in Germany, and be- 
 low the coal formation in England.' These writers (or rather Rev. W. D. 
 Conybeare, who wrote the article here referred to) regard the rothe todte 
 liegende of the Germans, as distinct from the old red sandstone of England. 
 ^uery — if the rocks along the Connecticut are really the coal formation of 
 Europe, may not the red sandstone east of the river in Chatham, East-Uart- 
 ford, Windsor, &:c. be the rothe todte leigende ; and that west of the river 
 the old red sandstone of England? 
 
 This same writer, speaking of the real coal formation, says that " at 
 least ten characters will be found in common between the carboniferous
 
 150 Geology, &/-c. of the Connecticut. 
 
 ^ P. S. Coal Formation. 
 
 Since the publication of the descripiion of this series of 
 rocks along the Connecticut, I liave had an opportunity to 
 examine more extensively than 1 had done before, the coal 
 foraiation of Rhode-Island ; and thus to institute a com- 
 parison between the two. And I feel satisfied that they are 
 very distinct from each other ; and that the Rhode-Island 
 formaiion is the oldest. There is a sort of general differ- 
 ence beiwet n them, which is readily recognized by the eye, 
 but which it is not easy to describe. In the Rhode-Island 
 rocks, however, there is a greater resemblance, in the gene- 
 ral aspect and in the fracture, to primitive rocks than in 
 those of the Comiecticui ; and the former are, in general, 
 harder and more compact than the latter; and their cement 
 is more argiliaceons. The coarse puddingstone, so abun- 
 dant inRoxbury, Dorchester, Sic. and which is seen at in- 
 tervals most of the distance to the anthracite beds in Ports- 
 mouth, approaches, in certain varieties, very near a similar 
 rock in ]\Iontague, Sunderland. Dui-Jiam, 4'C-- In the first 
 named rock, however, the cement is rather more abundant, 
 and the rock, as Maclure very happily expresses it, " l)as 
 the appearance as if the cement at the time of formation 
 Iiad a consistence sufScient to prevent the particles i'rom 
 touching each other." Certain fine red and coarse gray 
 slates occur in the two formations which can hardly be dis- 
 tinguished, except that those in Rhode Island (as well as 
 most of the other transition rocks there,) are traversed by 
 veins of quartz, but those on the Connecticut never are. 
 
 I would not be understood as endeavouring to prove that 
 the Rhode-Island formation belongs to the Wernerian trans- 
 tion class and that of the Conupcticut to the secondary. 
 Both probably are transition ; yet the one may lay claim to 
 a greater age than the other. 
 
 and traBsitJon class (of Werner) for ono ^'Inch could lead to an opposite 
 arraojjemeat" — that is wiUi the flcetz class, and also " that the sandstones 
 ol the lower part of this series approach closely m iharaclerto the more ob- 
 viously mechanifal varieties of 2;rey\vacke, and indeed so completely pass 
 into Ihut rock, that in many instances tiie limts between this ieries and 
 that of transition rocks, can onlv br arbitrarily assigned." — (pp. 323 and 
 324.)
 
 Geology, >^-c. of the Connecticut^ 151 
 
 Gneiss. 
 
 The more I examine the rocks in New-England, the bet- 
 ter convinced 1 am that the extent of this rock in this re- 
 gion, has been overrated by geologists. The truth is, that 
 almost in every place which I have examined, mica slate al- 
 ternates with gneiss, or overlies it. so as to occupy nearly, 
 sometimes more than half the surface. Hornblende slate 
 and granite, also occur in the same series. In passing from 
 Northampton to Boston, I have never found any gneiss east 
 of Worcester ; althouglvin going from Providence to Hart- 
 ford, this stratum occur^nly twelve miles from the former 
 place and continues with alternations of mica slate, inc. 
 to within a kw miles of the latter place. 
 
 I cannot avoid remarking here, that wherever I have 
 seen beds and veins of granite in gneiss and mica slate, I 
 have usually found the strata much distorted and deranged 
 in the vicinity ; and r?'ce versa, where derangement of the 
 slate appeared, I have generally been able to discover veins 
 or beds of granite. And wherever granite veins exist, gra- 
 nite beds are not usually far off. 1 might say more on this 
 subject : But it ha?»rjTyJPlc*ently attracted my particular 
 attention, therefore I desist. I am satisfied, however, that 
 many of the phenomena of Glen Tih are repeated in New- 
 England. 
 
 Greenstone — primitive — transition and secondary. 
 
 The second supposed distinction between the primitive and 
 secondary greenstone of the Connecticut is very imper- 
 fectly stated page 32 ^Hjgf^ The mere fact that the primi- 
 tive greenstone forms beds in other rocks does not distin- 
 guish it from secondary greenstone ; since this occurs in the 
 same situation. But the former, at the sides of the bed, 
 passes by imperceptible gradations into other rocks, such 
 as greenstone slate, chlorite slate, &ic. thus excluding the 
 idea that it could have been forced in between the strata of 
 other rocks after their consolidation : whereas the latter 
 rock is distinctly characterized to the very line of junction 
 with the sandstones and puddingstones, unless there be a 
 slight chemical changeo few inches on either side of this line^ 
 as if bv heat.
 
 152 Geology f ^t, of the Conntcticut. 
 
 It may not be amiss to state here that the greenstone of 
 the Connecticut has a very different aspect internally and 
 externally from the epidotic and sienitic greenstones in the 
 vicinity of Boston. The latter are evidently transition, be- 
 ing associated with the sienite. porphyry, gray wacke, argil- 
 lite, &ic. But I am not prepared to state precisely in what 
 respects they differ from the greenstone of the Connecticut. 
 
 And although it does not strictly belong to this place, it 
 may not be amiss to refer to the intrresting dykes of basal- 
 tiform greenstone occurring in sienitic granite in the vicini- 
 ty of Boston, of which I do not recollect to have seen an 
 account. 1 have noticed them in Midbury and Weymouth 
 in real granite — that is, the rock was destitute, at the place 
 of hornblende. One in Weymouth, or perhaps in Brain- 
 tree, I traced several rods, and it retained its width with 
 mathematical exactness, and the sides were perfectly 
 smooth. These dykes deserve more examination and bet- 
 ter description. Perhaps some of them contain real basalt. 
 
 White Augite. 
 Since writing the account of this mineral found in Go- 
 j,. shen, which occurs on page^lft 03l^. 1 have visited the 
 
 ^^^ locality again, and find it in imiTiense abundance. About 
 
 two miles north of Goshen meeting house, a {e\v rods be- 
 yond a tavern on the west side of the road, is a pasture al- 
 most covered by bowlders of granite. These bowlders are 
 full of augite, some of the crystals of which are from twelve 
 to eighteen inches long and three or four wide, although 
 they are very imperfect. Every cabinet in the world might 
 be supplied from them. I noticed also in the same rock 
 some crystals of beryl more than^^|(jjfch in diameter. 
 
 Precious Gernet. 
 This occurs abundantly in gneiss in west and south 
 Brookfield. Some are an inch diameter ; their colour is 
 }ight poppy red, and it is rare to find any exhibiting the 
 form of the crystal distinctly, so that perhaps they ought 
 to be referred to pyrope. 
 
 Prismatic Mica 
 Found in the northern part of Williamsburg in granite. 
 Good specimens may thence be obtained.
 
 Muf Species of Botrychimu 1 53 
 
 The annexed drawings are from the same plates, as those in- 
 serted in Vols. 6 and 7 of the American Journd of Science. 
 And it so happens, th't a few figures, not belonging to this 
 Sketch, could not be omitted. Among these, is a new species 
 of Botrychium, found in Conway, and fully described in Vol. b, 
 p 103 of Journ. Science. It was thought, that it miglit not be 
 vnacceptable, to insert the following short description ot this 
 plant, in this place. 
 
 Specific Character. 
 
 Botrychium Simplex : ^nd simple, 5 lobed, or 3 cleft ; 
 segments unequal ; spike subi-compound, interrupted, unilate- 
 ral, be-^ring sessile capsules, in the last part of June, of the size 
 of a mustard seed. Nearly allied to JS. ZuHaria of Europe : 
 but itdiifers, in having a simple leaf, a spike hardly compound, 
 and much larger capsules. In a dry, hilly pasture, a few rods 
 south of the residence of Col. Charles E. i3illings, in Conway. 
 
 Corrigenda. 
 
 The author of the preceding Sketch had not an opportunity 
 to examine the proof sheets, and a considerable number of er- 
 rors have been found, particularly in the first Part. Those, 
 however, affecting the sense, have been corrected by the pen, in 
 the few copies, that have been printed in this form 
 
 It is but justice to himself, also, for the writer to remark, that 
 a pressure of more important duties has prevented him from 
 giving that attention, in the preceding Sketch, to the graces of 
 composition, which would have been desirable. He had been 
 for several years collecting fa^ts, relating to the Geology, &:c. 
 of the Connecticut; and the alternative seemed to be before 
 him, either to abandon them to oblivion, or to publish them in 
 the rather imperfect form in which they are presented in the 
 preceding pages. He has chosen the latter course ; whether 
 wisely, or not, it is not for him to decide. He will be satisfied, 
 if the facts exhibited should render any service to a science, 
 which has recently assumed so interesting a relation to revealed 
 religion. 
 
 The term stratification has been used in the geological part of 
 the preceding Sketch, in a (ew instances where most geologists 
 would probably have employed schistose or slaty. Some re- 
 laarks of Greenough, in his work on the First Principles of Ge- 
 ology, led to this blending of the terms. 
 
 The term alluvial, in the preceding Sketch, is employed in 
 the same sense, in which it is used bj all American writers.
 
 154 New Species of Botrychiutn. 
 
 But, in Europe, it has recently been very much restricted in 
 its signification. According to this limited view, but very little, 
 that is marked on the Bccompanying map as alluvion, is really 
 such ; only a few small basins, as that of Farmington, West- 
 field, Deerfield and Northampton, which are annually overflow- 
 ed by rivers. The remainder corresponds, probably, to some 
 one of the older European formations : perhaps to the London 
 clay.
 
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