“a VL heyy Yi Le eM Lie “LY a tibe a zy Hap : fe si, ae «en ge 2 LOLOL OODLE TOLLE YL Vy, VEEL her +f “if . t d nhs " ’ Z : Wy ees oh] ' q , ¥ ’ 1 ie er 4 ; j ‘ ; “- = t re ‘ ~ ’ ~ cy ‘ sf ‘ . . . \ iN Bes University of the State of New York New York State Museum 51st AnnuaL Report OF THE Bits EN 1S 1897 VOR 2 REPORT OF THE STATE GEOLOGIST AND PALEONTOLOGIST AND FIELD ASSISTANTS ‘TRANSMITTED TO THE LEGISLATURE 24 MARCH 1898 ALBANY UNIVERSITY OF THE STATE OF NEW YORK 1899 mus 1873 Martin i Townsenp, M. A. LL. D,. . 6a 1877 Cuauncry M. Drerrw, LL.D. te na : 1877 Cuaries E. Firon, LL. B. M. A. ats H. D. "1883 St Oram McKexway, LL.D. L.H.D. D.C.L. - Brookl - 1885 Hamitton Harris, Ph. D. LL. Di So _ 1885 Dance. Boaca, Ph.D. LL.D. =. oe Oe?) 1888 Carrot, E, Surru, LL.D. -. > = - § = 1890 Puy T. Sexton, LL. D. a a" on 1890 T. Guirrorp Suir, M. A. CO. E. LE D. = 1893 Luwis A. Srmson, B. A. M. ‘D. — = 1894 Syitvestpr Matonp - - See gs = 1895 Areerr Vanprer VEER, M. D. Ph. Daas Me Jah 9D CHARLES R. Skinner, M. A. LL. D. rae ee 4 Ri | ae of Public Instruction, ex ‘ off ec, SECRETARY Mervit Dewey, M. A. DIRECTORS OF DEPARTMENTS 1888 Mervi. Dewey, M. A. Administrative, State libr | Home education | 1890 Jamus Russet Parsons sr, M.A. College and High hae dep’ ts se ‘a im _ 1890 Freperick J: Hy, Mirrinn, Phi DD: Stateanuseurae Po + -etroleum and natural gas in western New York: by Plane Bishops. 5.5.0)... Wy. tae oa de ile cota ole’ 1s okcro Ue ee sssification and distribution of the Hamilton and Chemung series ;of central and eastern New York, re 2: Dy eae Q pis Ne Ge lq (eVel ve yer,-e) vw: e@: 6!) Sk ehie) ice fa, ee) je).00 ley oe M840!) (0) @ fe) we Lieilis eee ee © © © eo we we ww eee ee BP we Cm aranep eusehner eet. (syne diene aie se! s 6.8/1.0 © ee eee + See we a ew © Pr Y eee Cee ee Sel 6 fa) lefiten au 9)! * e\selie es 6, 0 a) ee. @ 08 . ececee ses «+e ee ee we ee etait tee, feaxrsorian ss '/z ne / Ns : QO) wo oe TPO) ROE To His Excellency FRANK 8. Buack Governor of the State of New York p: Sir: The operations of this department during the past year _ have been in continuation of the work of previous seasons along : ; of the state and b) the perfecting of the geologic map of the state. % It seemed important that at the opening of the field season im- : y mediate attention should be directed to the mode of occurrence of ,this natural product. The striking of rich supplies of gas _ in the vicinity of Rome, Syracuse, at Baldwinsville and in Os- Wego CO., in addition to constantly increasing operations in and storage of natural gas and the possibility of the development < the more western and southwestern parts of the state, rendered the following lines: a) the exploitation of the economic products a it imperative that measures be taken at once to accumulate and ‘= conserve the important data that these numerous deep wells : . were affording. "The work previously undertaken in this direc- tion has been incomplete and, though important in having put on record the logs of many wells, giving the succession and thickness of geologic strata, has been altogether insufficient to establish any explanation, or to formulate a law of the mode of a Such investigations will not be undertaken by private individ- f uals for the reason that, though their results may be of profound _ ultimate effect upon the development of the mineral wealth of _ the state it may not be possible to convert them at once and without delay into dollars and cents. Hence all states of ad- vanced ideas, where such accumulations of natural gas, petro- a : and other mineral products are known to exist, have made 4 on storage of natural gas and the method of location of paying wells. ~ as well as in other countries.@ Osc: NEW YORK STATE MUSEUM what circumstances such natural supplies can be most advan- tageously exploited, and have given substantial reasons for such determinations. To carry on such work in this state a smail : appropriation was asked of the last legislature and granted by it, but was vetoed by the governor on the ground that such operations should be conducted by private individuals, which, as above remarked, is manifestly impracticable. With full reali- zation of this impracticability, the work was inaugurated with sh such appropriations as this department had and in order to carry it on, a necessary curtailment of expenses has been made in other directions. | | I have the honor therefore to present herewith the very valu- able report on this subject by Prof. Edward Orton, the state geologist of Ohio, who has for vears made this a subject of special study and is recognized as the foremost authority upon it in this To enable Prof. Orton to cover the entire gas field of the state in one season he was given the assistance of Prof. Irving P. Bishop, of Buffalo, who has taken special charge of the gas and oil fields of western and southwestern New York and has sub- mitted an interesting and important report upon the result of his investigations. In my report for 1895, Prof. Charles S. Prosser, of Union col- lege, gave the results of his study of the Hamilton and Chemung. formations in central New York. This report was but a pre- liminary statement of his results and the present report con- tains the outcome of his continued study of the distribution of the same formations in the more easterly portion of the state. This work of Prof. Prosser is of high value as it affords data for an entirely new line of division between the formations, which has for years been a matter of great obscurity on account of the homogeneity of these sediments and the slight variation of the characters of the fossils which they contain. aln order to secure for Prof. Orton’s important paperamore general circulation than it could obtain through the medium of this report, it has been deemed best to issue it separately as a bulletin of the state museum. Therefore it does not appear in this report but will be found incorporated with the museum report for the current year [1899] and as Museum bulletin 30. September, 1899. JOHN M, CLARKE RERORT OF GEOLOGIST AND PALEONTOLOGIST, 1897 7 During the past season Professors James F. Kemp, of Colum- pia university, C. H. Smyth jr, of Hamilton college, and H. P. Cushing, of Adelbert college, Cleveland, O., have continued — es their operations in the Adirondack region of crystalline rocks ’ and the first two gentlemen present herewith reports of their work, the former in Essex co. and the latter in the western part of the Adirondack region. Prof. Cushing’s results will be a incorporated in a future report. = Dr Heinrich Ries, of Columbia university, has been employed - to make a special study of the limestones of the state with refer- ence to their various economic values, and his report is herewith submitted. ‘ Mr Clifton J. Sarle, of Rochester, was sent into the field for the purpose of collecting specimens of fossil sponges to be used in the completion of the monograph of the Dictyospongidae, - the final part of which was transmitted with my last report. Mr — Sarle succeeded in securing alarge amount of material in Steuben co. and visited the southern parts of Tioga and Broome counties — for rare species of these organisms and from there was de- tailed for a short time to trace the outcrops of the upper layers of the Niagara formation in the vicinity of Rochester. Thereafter he was sent into Clinton co. for the collection of fossils in the Chazy and Calciferous limestones, in which work he was engaged for about one month. Later in the season he was engaged in the _ Chemung rocks near Avoca, in the collection of the crinoids of _ that formation, in this case with satisfactory results. “This report also contains a paper of much interest which has been communicated by Prof. Charles S. Prosser, of Union college with Mr R. B. Rowe, one of his special students in geology. It is entitled: the Stratigraphic geology of the eastern Helderbergs. Very respectfully JAMES HALL p 1 State geologist and paleontologist _ State Hall, Albany, Mar. 24, 1898 \ REPORT ON TROLEUM AND NATURAL GAS IN _ WESTERN NEWYORK By Irvine P. Bisnor VWeky, respectfully Irvine P. BisHop i SCOPE OF THE WORK i, _ The original purpose of this investigation was to ascertain the Ri geology and Stet ubion of natural a along the outcrops of the 4 ah The Dadi accumulation of data from localities outside the bi _ proposed field, necessitated an enlargement of the scope of in- -quiry So as to include all of western New York exclusive of the 3g southern tier of counties. Later on the work was extended so as p to: cover Cattaraugus co. oe to ent the geology and dis- Wells in Cayuga county Weedsport Oe: Only two wells are reported ‘from this co. The first of these was bored at Weedsport previous to 1873. The total depth _is said to have been from 600 to 800 feet.? No gas of any impor- _ tance was found. ‘gate : Auburn Sean the latter part of 1897 a well was sunk at Auburn, N. Y., starting on the lower part of the Corniferous limestone. The fol- lowing record is furnished by Mr L. B. Cary, driller, and by Mr J. W. Stearns, contractor. - aSee Report of sup’t N. Y. salt reservation. 1873. 4 | Record of a well. Be. As Salt water - at 685 feet Struck gas” Sigg te as Cased off 645 White Medina sand ne Soft ‘shale to 1025 Red Medina sand spans ‘Niagara limestone 1025 White Oswego sand © Black shale 1100 Black shale; 72598 Blue shale 1310 Trenton rock Clinton limestone 1520. Stopped drilling a Red Medina sand 1538 | gas was found in 1 the ‘a of. the Helo aad the bottom ie h Genesee. ze \ A small streak of sulfureted hy greeny also, occurred i 8 : Wells in Seneca county ees aM See Seneca Falls per | a Since 1885, 12 wells have been sunk at Seneca Falls, N. : - depths ranging from 1500 to 3560 fect. The following _ record of well no. 12 was furnished by Mr W. A. Hoseley. Drive pipe to limestone 77.feet Gray shale mixed with — Sa, aoe et z = 4 ee oe Eas ~ & Roser artes a gees, PS. fi 3 _ Top of salt sand at 305 black ‘Bottom’ of salt sand | 455 Half black shale mw top ot big: red shale 485 All black shale - Bottom of big red shale 675 Shale and lime mixed Cased to- | 513 All shale a: pak Stn Niagara 710 Top Trenton ae iy _ Top Clinton OSB Black shale , ‘ oe _ Top Medina | 1205 Limestone Ae Flow of gas, enough to Nearly all black shale’ way an light 1254 Crystalline limestone Gray Medina (?) 2030 All black shale aoe ; ua Red Medina 2140 Limestone with white eee AN pray |: 2175 streaks | : To bottom confined rock pressure of 500 pounds. The best gas was to about 500 feet below the top of the Trenton limestone. In this respect the well behaves like the famous Kelly well at Zoar near Gowanda, N. Y. , _ The other wells strike the rie sandstone at ake! 1400 Bey ing rock. The specimens of sandstone brought up by the sand- _ pump from the gas rock at Seneca Falls, and also at West Bloom- _ field and Caledonia, were invariably red and generally extremely : hard. The gas horizon in these wells is by no means constant. in most cases it lay from 150 to 200 feet below the top of the Medina. Small quantities of gas also occurred in the same for- | cin ee group the earlier es are now yielding better than 4, those drilled recently. ies ‘The gas from these wells is piped to Seneca Falls where it is ’ used for heating purposes. The company which distributes it vik _ has about 50 meters set and supplies an average of 50,000 cubic Wells in Schuyler county Watkins a Near the sanitarium at Watkins a well was sunk about 20 years ago to the depth of 1530 feet.* There is no record or even tradition that gas was found in any quantity. When the well was completed it was plugged at two or three points and aban- - doned. A few years ago the upper part of the well was cleaned a It is reported that the drill stopped in black shale. x. i 14 NEW YORK STATE MUSEUM out and at once filled within 300 feet of the tep with mineral as water, which has since been utilized at the sanitarium for baths. | In June 1897, just after the slight earthquake shock which was ’ ee felt in western New York, the engineer noticed that the odor -. lo WA, of gas was increasing at the mouth of the well. - A meter was attached and registered a flow of 3000 cubic feet a day. The well was then pumped to 850 feet when the press-_ ure rose to 100 pounds and the flow increased to 10,000 cubic ie feet a day. In August 1897 the well was supplying fuel for cen the pumping engine and for the large range in the sanitarium . kitchen. Though the increased flow of gas mentioned above may have _ ee been caused by seismic disturbance, it is more probable that it . was due to diminished water pressure in the well caused by ex- * cessive pumping. Wells in Ontario county Geneva At Geneva a well was bored in December 1885 to the depth of ee 1100 feet. No gas was found, but a copious flow of mineral water — now fills the well and supplies the baths of the Sanitarium. No oe record of this well has been preserved. West Bloomyield - The first well in western New York to produce gas in paying quantities was sunk, according to Prof. Charles S. Prosser, in ' West Bloomfield township about 1863-64.¢ This is reported to have given in a still atmosphere, a 30 foot flame from a five inch pipe with an estimated daily production a 400,000 cubic feet. A line of wooden pump logs was laid from the well to Rochester and connected to the gasometer of the local” gas company with the intention of supplying both fuel and light- — ing. Water and mud entering through loose joints between the logs effectually closed the line after a few days and it was aban-— doned. Prof. Lattimore, of Rochester, informs me that, while it lasted, the gas was used for fuel in at least one of the hotels. a See C. E. Ashburner Petroleum and natural gas in New York 1888. p. 42. Also American jour- nal science and arts (2) 49: 336-37. #5 - PPTROLEUM AND NATURAL GAS IN WESTERN NEW YORK 15 Be find their gas in the lower part of the Marcellus shale. In 1894-— _ 95 two deep wells were sunk to the Medina sandstone in the 2" vicinity of Gates’s mills with the hope of increasing the supply Pee of gas from a lower horizon. One of these proved barren; the _ __ other gave a flow of about 100,000 cubic feet daily at a depth of a 2100 feet. The gage broke at 600 lb., the limit of Bee _ go that the full rock pressure was net ascertained. Of the shallow wells, one gave at the start 100,000 cubic feet of gas a day with a maximum confined rock pressure of 30 an ‘pounds which later fell to 18 pounds; 10 or 12 wells gave 40,000 cubic feet or better, and the others 20,000 or less with a pressure ‘ranging from 30 to 18 pounds. The gas is now piped to the villages of North and West Blapae field and to Honeoye Falls. The Ontario improvement and gas co., limited, owns the plant _ and supplies 200 stoves during the year, but not all at one time. : - At present the wells furnish barely enough gas to meet the , f demands of consumers. In J anuary 1898 a new well was drilled, - but failed to increase the supply materially. ‘The records of nearly all the borings in this field have been placed at my disposal by Mr S. Miner Wellman of Friendship, | _N. Y. and by Mr Isaac E. Dean, who drilled many of the wells. e The following show the characteristic conditions observed here. 3 Record of deep well s. e. corner of lot 54, two miles north of Allen | Hill, in West Bloomfield township | | Pocket of gas at 481 feet Bottom of Niagara (?) at 1770 feet ei ss Hard rock (Corniferous?) 450 First show red rock 1815 Through hard rock 590 Top of Medina sand- _ Onondaga (?) 960 stone (?) 1860 Salt mixture 1193 First gas 1945 Clear salt (9 ft) 1218 Gas, main flow 1955 Cased to _ 1307 Bottom of well 2042 Small streak of salt 1510 ates 16 NEW YORK STATE MUSEUM The interrogation marks are my own; the other records are : those of the driller. The red rock at 1815 feet is probably the ~ oP of the Medina. | , Second deep well, near the first p Shale gas at 380 and 457 feet Red rock 1800 feet Gas producing 30,000 cu. Cased to 1317 ft a day 490 ' Yop of shell 1840. Hard rock gas 805 Gas 1948 The gas at 805 feet was very abundant in both wells but did not last. Worthington well, no. 1 Located on high ground one mile north of Allen Hill. ‘Record from Mr I. E. Dean | Drive pipe 98 feet Light gas 415 to 480 feet First gas 168 Best gas 472 to 484 Cased to 200 A little gas , 476 Light gas at: 8335 Black rock (Marcellus) 519 Light gas (shot) 857 to 367 Bottom of well 525 Worthington well, no. 2, lot 45 ' Bed rock at 32 feet Water at 170 feet Limestone to 36 Chocolate slate 185 Large vein water 95 Gas 400 to 410 Cased in chocolate rock to 105 Shells 424 Dark chocolate slate 124 - . Finished 447 Slate 140 Shot 400 to 447 feet Worthington well, no. 3, lot 46 Bed rock at 81 feet Cased at 201 feet — Chocolate shale 110 Good gas 378 Cased at 185 and 170 Light gas 418 Hard shell 190 Bottom of well 453 H. Arnold well, s. w. cor. lot of the townshp Bed rock at 80 feet Gas at 290 feet Slate through first Shell 412 chocolate 156 Shot 430 Limestone (?) 171 Gas at 800, 812 and 860 Water 172 Gas increased to 890 Cased to 183 When the flow was very large.. _ nF cee —_— Se a 9 ey eee = PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 1% This well gave 120,000 cubic feet and was the best shallow well in the field. Pierpont well, lot 35, south of Allen Hull - Drilled April-June 1889 Bed rock at 6 feet Lighter chocolate shale at 870 feet Iron pyrites 107 Light gas 380 Light colored shale 115 Good show of gas 394 Chocolate colored shale LG White lime shell 400 Big vein water 200 Dark chocolate shale 412 Cased to 205 Water 574 First gas 209 Shells full of gas 628, Lime shells 224 683 and 660 Lime shells 260 Black (Marcellus) shale 680 Chocolate shale 318 Limestone (Corniferous) 733 Gas 828 - Finished 782 Thompson well, no. 2, lot 54, West Bloomfield Bed rock at 53 feet Third gas at 315 feet Cased to 71 Finished, top of Cornif- First gas 104 erous 414 Second gas 140 ; Lee well, no. 1, one fourth mile north of Gates’s Mill First well drilled about 1871. Record from Mr I. E. Dean Bed rock at 10 feet Second gas 880 to 365 feet Cased 97 Finished at 418 First gas at 230 This well was a good producer and did not reach the Cornifer- ous limestone. Lee well, no. 7 Drive pipe . 60 feet Second gas 188 Casing 140 Completed at Corniferous 460 First gas . at 123 Well barren. Rollins well, no. 2, lot 6, West Bloomfield Located on a hillside Drift 194 feet Total depth 495 Small show of gas 415 Well barren. 18 NEW YORK STATE MUSEUM Rollins well, no. 3 To rock 27 feet Limestone 420 First gas 295 to 310 Second shot 455 First shot at 300 Finished at 475 /) Rollins well, no. 6 Cased to 99 feet Fourth gas 330 First gas at 140 Finished, above Cornif- Second gas 268 erous 438 Third gas 300 Fair. McAllister well, no. 2 Bed rock at 75 feet~ Third gas (shot) 430 First gas 165 Fourth gas 475 Second gas 210 Finished at Corniferous 504 McAllister well, no. 4 To rock 36 feet Gas 730 to 746 and also 780 First gas 431 to 441 Salt water 784 Limestone (Cornifer- Gas, strong at 820 ous ?) at 455 Gas, increased 835 Gas at 484, 505, 545 and 576 Fresh water at bottom Gocd gas 696 of well 855 McAllister well, no. 12 Bed rock at 386 feet Center of shot at 428 First gas 431 Finished at Corniferous 441 Well barren. Emerson well, no. 5, McAllister farm, Gates’s Mill Record from Mr I. E. Dean Drift 48 feet Chocolate shale, with a First gas at 137 little gas at 415 Second gas 345 Biack shale 415 to 452 Gas from 870 to 381 Corniferous limestone at 452 Black shale at 410 Case well, no. 2 Bed rock at 12 feet Corniferous - at 448 First gas 385 Drilled into limestone + Second gas 428 Third gas 448 To tabiye cviare ie ct eile ie te 452 feet feet feet feet feet PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 19 Well shot at 385 feet increasing the flow of eas. A second shot at 425 feet was unsuccessful. This was one of the best of the shallow wells. Case well, no. 8, one mile north of Allen Hull Record from Mr I. E. Dean Bed rock at 77 feet Finished above Cornif- Gas and water, 90, 148, erous at 517 feet 171, 188, 212, 247 and 3383 Well torpedoed with 15 foot shot between 457 and 475 feet. The top shot at 457 feet was unsuccessful. The lower shot pro- duced a good flow of gas. Johnson well, Richmond township, one mile n. e. of Allen Hill Record from Mr I. E. Dean 7 Bed rock at 28 feet Fourth gas at 512 feet Red shale 175 Shells 527 Cased 228 Fifth gas 532 First flow (pocket) 229 Shells 537 Second gas 360 Sixth gas 538 Best gas 492 First shot 492-507 feet. Second shot 5238-538 feet. Morrow well, no. 1 ' Bed rock at 26 feet Shell at 190 feet Chocolate rock 430 Gas, good 381 First gas 130 Gas (shell) 403 Second gas 146 Gas, good 430 Slate 180 Bottom of well 468 Shot at 430 feet. Norgate well, lot 51 (Richmond?) near center of township Bed rock at 17 feet Slate at 398 feet First gas 30 Shell 670 Black rock 30 Gas 681 Chocolate rock | 78 Black rock 706 Shell and more gas al amtrnc: Shell 726 Light slate 120 Limestone 736 Chocolate 340 Finished 741 Cased to 342 Shot 660-675 20 NEW YORK STATE MUSEUM The principal gas horizon of the shallow wells is in the lower part of the Marcellus shale, and near the Stafford limestone. While in a number of cases gas has been found above the Staf- ford horizon, the weight of evidence goes to show that the gas originates in the densely bituminous black shales at the base of the Marcellus and is held in by the limestone which serves either as a cap where it is continuous, or as a reservoir where it contains loose joints and fissures. The pocket of gas at 805 feet in the deep wells appears to be too deep to lie in the honeycombed “ bullhead ” waterlime at the top of the Salina group, and is probably a small inconstant horizon. There is nothing in either the records or in the drillings preserved to show that the white or ‘“‘ quartzose ” Medina sandstone exists here. The gas rock in the Medina, as shown by the drillings, is a nearly pure, compact red sandstone having the usual characteristics of the Medina of western New York. _ Vincent At Vincent in the town of Bristol a well sunk in 1865 fur- ‘nished a small amount of gas which apparently came from the Marcellus. The borings at Canandaigua, Clifton Springs, Naples and elsewhere in Ontario co. have produced no gas of any impor- tance. From the Canandaigua lake region C. A. Ashburner reports petroleum in several wells, one of which is said to have pro- duced five barrels a day. This report I have not been able to verify. Wells in Livingston county Avon The following record of a well at Avon in the northern part of Livinston co. is furnished by the driller, Mr Frank Westcott. Top of Corniferous at 170 feet Gas - at 1463 feet Top of Niagara 875 Depth of well 1520 Top of Medina sandstone 1400 The maximum closed pressure is reported to be 500 lb. The daily production was not ascertained. PHTROLEUM AND NATURAL GAS IN WESTERN NEW YORK Dah Caledonia At Caledonia six wells have been drilled by Mr. J. C. Tennent and another is now (Jan. 1, 1898) under way. No record of these was kept until the Medina sandstone was reached. Mr Tennent. has furnished me with the following facts regarding the best well. Elevation of well mouth Top of Medina sandstone 16s is 560 feet at 997 feet Drive pipe to (Cornifer- First show of gas 1010 ous limestone) 78 Second show of gas 1069 Casing to shut off salt Pay gas 1085 water 472 Through gas sand 1098 Red shale at 987 Depth of well 1119 Stopped in red shale. Well finished Nov. 12, 1895. The confined gas pressure was 400 pounds with a flow of ap- proximately 150,000 cubic feet a day. The other wells showed no marked difference in the nature or thickness of strata except that in three the sandstone was but 75 feet thick, the lower sand being replaced by red shale. As the lower part of the sandstone is the gas horizon, these wells were nearly barren. | | The other producing wells yielded at the start approximately 3000 cubic feet a day with an initial pressure of about 175 pounds. The gas from these wells supplies 65 connections in the village of Caledonia. Among them are the village water-works and several large, establishments using power. Batavia Record from Prof. Charles 8. Prosser Altitude 889’ A. T. Depth Thickness 40’ Drift 40’ rE, 60’ Marcellus 22 NEW YORK STATE MUSEUM Depth Thickness , Upper Helderberg 150" Lower Helderberg 250’ —- 500’ About 15’ rock salt at 6:0’ 1 Coos Salt group 750’ —— 4 Top of Niagara limestone | 500° Niagara 1000’ — Clinton (?) 100’ Probably mostly Medina 1100’ —— Medina 900° Bottom of well in Medina 2000’ a Of the 150’ assigned to the Helderberg formations it is probable that, as in other known sections in western New York, 100 feet : should be considered Corniferous and the lower 50 feet of water- lime should be classed as the upper part of the Onondaga group. The Clinton, which Prof. Prosser doubtfully assigns to the 10007 horizon could hardly have been represented among the samples from which the record was compiled. In the Corfu well, which agrees in its general features with others in western New York, the Niagara limestone is reported to be 250 feet thick with 70 ~ feet of shales below. The Clinton limestone is 30 feet thick with a thin underlying band of olive shales, the latter averaging about five feet. As no sample was taken between 1000’ and 1100’, the Clinton was probably overlooked. Wells in Genesee county Le Roy ‘ Mr. J. C. Tennant has drilled a well on the Monroe farm, one mile east of the village of Le Roy, Genesee co. The elevation of this well above tide is 690 feet. The Medina sandstone was found at 1025 feet and proved to be 75 feet thick. A small showing of gas was found in the upper part of the sandstone, but was not enough to be of any use. The well was completed in red shale at 1200 feet. | PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 23 In the original well bored for salt at Le Roy, February 1879, a small pocket of gas was found at 450 feet. None of the wells since drilled in that vicinity have found any gas worthy of record. Corfu At Corfu, in Genesee co., five wells have been drilled, four of which are nearly in a north and south line at an average distance of 1000 feet apart. In two of these the original confined rock pressure was 400 pounds, and in another, well no. 4, the gage showed 500 pounds pressure after one night. Well no. 5, com- pleted during the autumn of 1897, is reported by Mr J. W.Stearns, the contractor, to yield 250,000 cubic feet a day. This last well is located near the Lehigh railroad tracks at the extreme southerly end of the group, and is the best well yet put down. The gas is piped through the village of Corfu, and in August 1897 supplied 108 connections. Water in two wells has caused decreased pressure, but there appears to remain a supply ample for the needs of the village for years to come. The geological conditions occurring here are shown by the fol- lowing record furnished by Mr J. W. Stearns. Well no. 1, Corfu Marcellus shale 30 feet Niagara shales . 10 feet Flint (Corniferous) 180 Clinton 30 Limestone and shale 458 Medina sandstone 110 Niagara 250 Red shale 20 Wells in Wyoming county. Attica The first deep boring in this vicinity was an exploration for salt in the later part of the year 1883.9 Not finding salt in pay- ing quantities, the well was continued down to 1960 feet, about 240 feet below the top of the Medina group, without getting any show of gas. In September 1897 a well was sunk for Hon. F. C. Stevens about 400 feet west of the original boring. The well is a See Report N. Y. state geologist. 1898. 6 See author’s paper in report N. Y. state geologist 1885. 24 NEW YORK STATE MUSEUM located near the edge of a deep preglacial valley now filled with drift, the mouth being approximately 990 feet above tide. The following record was furnished me by the contractor, J. W. Stearns. Stevens well, no. 1 f, Completed Sep. 14, 1897 Drift 204 feet Niagara limestone at 1475 feet Shale (Genesee (?) and Black slate 1570 Hamilton) to 550 Clinton 1605 Corniferous limestone Medina sandstone 1704 160 ftto 710 Red shale to bottom Limestone and _ shale of well> 4 mixed to 1050 — Black and red shale 1250 Total depth“. 2. eee 1708 First gas at 1658 feet Third gas at 1690 feet Second gas 1672 Mr Stearns reports the original confined rock pressure as 650 pounds with an estimated (but not measured) capacity of 400,000 cubic feet a day. The gas from this well is now piped through the mains formerly used for illuminating gas and supplies about 100 connections. At the time of my visit, Jan. 8, 1898 the gage registered 220 pounds at 4 p. m., an hour which would represent a fair average of use between sunrise and sunset. The superin- tendent in charge said that the pressure rose during the night to 480 pounds. Three other wells have since been sunk, two of which belong to Mr Stevens and the third to Mr Benedict. Stevens well no. 3 on the Flach farm west of the village has, according to Mr Stevens a confined rock pressure of 620 pounds. The well has not been metered, but is roughly estimated at 200,000 to 250,000 feet a day. It is reported that Stevens well no. 1 passed through about seven feet of rock salt. . In the numerous borings for salt throughout Livingston and Wyoming counties, gas in any quantity has been generally ab- sent. Enough gas for two stoves is reported from one of the Kerr wells at Rock Glen, Wyoming co., apparently from the Ham- PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 25 ilton shales. In the well at Dansville, Livingston co. small streaks of gas were found at 295 and 508 feet respectively.” In both instances the gas was found at too high an elevation to have come from the Marcellus shales, and it is therefore quite certain that this horizon -is not productive of gas in the counties under consideration. As the borings for salt seldom penetrate to the top of the Niagara limestone, they are too shallow to reach the lower horizon from which gas is generally derived. Arcade At Arcade, in the southwestern part of Wyoming co. near the Cattaraugus co. line, four or five wells have been drilled of which no complete record has been kept. In the well located on the M. J. Stearns farm and drilled by John Smith of Ormsby Junc- tion, Pa. the following conditions.were found. Drift 110 feet Gas sand, 14 feet at 730 feet Shut off fresh water. at 290 Gas sand, 24 feet . 2200 Shale to 750_ Salt water 2405 which filled the well and flowed. The gas sand at 730 feet furnished a pocket of gas sufficient to run the boilers two days. The well was finally plugged at about 2250 feet and shot at 2200 feet with 70 quarts of nitro-glycerin, giving a fair flow of gas. Two years and four months later it gave a measured flow of 1100 feet of gas a day. The above record was furnished from memory by a gentleman interested in putting down the well, and is probably only ap- proximately correct. Wells in Erie county Very little drilling has been done in this county within the two years: which have elapsed since my last report. In the latter part of 1897 and in January following, the Buffalo cement co. put down two new wells near their works on Main st. One of these gave an output of 25,000 cubic feet, and the other not more than 3000 cubic feet a day. The Buffalo natural gas fuel co. is now (February 1897) sinking a well at Ebenezer in the South Buffalo field. aC.S8. Prosser, Thickness of Devonian and Silurian rocks of western N. Y. p. 74. 26 NEW YORK STATE MUSEUM Two wells were also put down in the Canadian field near Crys- tal Beach about a year ago, but did not give a profitable yield. No geologic facts of importance have been brought to light by any of these borings. , At North Collins, about 17 miles southwest of Buea in an air-line, a well was put down during the latter part of 1897 to a depth of 1800 feet. The mouth of the well is about 100 feet be- low the lowest Portage sandstones and approximately 830 feet above tide. I was told that samples from every screw of drill- ings had been preserved, but access to them was not allowed me. Mr H. D. Auerbach, one of the company engaged in ise down the well, gave me the following data. Shale to Corniferous Shales to bottom of limestone 1028 feet well at 1800 feet Limestone to 1240 Salt water at 1800 I visited the well Nov. 27, 1897 and obtained a sample of the drillings at 1800 feet. They were very hard limestone, effer- vescing slightly in cold and dissolving rapidly and almost com- pletely in hot hydrochloric acid. From its position and charac- teristics I was satisfied that the rock at the bottom of the mee was the top of the Niagara limestone. At the time of my visit the well was furnishing enough gas for the boiler. In the following week the well was shot with 80 quarts of nitro-glycerin at the base of the Corniferous, or more probably in the “ builhead ” waterlime at the top of the Salina, securing an increased flow of gas, the quantity of which I could not ascertain. The well had not been metered Feb. 22, 1898, and the estimates obtained from different members of the company owning the well varied from 10,000 to 2,000,000 cubic feet a day. If the above stratigraphic data are correct, they show that the limestones of the Corniferous and Upper Salina are here 60 feet and the Salina shales at least 150 feet thicker than in the northern part of the county. Of the well at New Oregon, eight miles east of North Collins, no record has been obtained. A well is now in process of drilling on the House farm between Springville and Zoar. PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 27 NORTHERN TIER OF COUNTIES The following records collected from various sources show the thickness of the strata in the counties bordering on Lake On- tario from Cayuga co. westward. With the exception of the Clyde well, the borings start upon the Medina outcrop or upon the northern edge of the Niagara, and all penetrate the Trenton to a greater or less extent. As will be seen, gas occurs very sparingly throughout this strip. Wells in Wayne county Clyde Altitude approximately 389’ A. T.4 Gray, green and blue Medina red shale 24 feet marls with gypsum 152 feet Greenish, gray, silice- Red marls 156 ous sandstone, the Blue and green marls “Gray band ” S (Salina ?) on Red shale alternating Dark blue limestone, with red sandstone upper div. of Niagara 110 forming the red Shaly limestone of the Medina 915 Niagara 225 Oswego gray sandstone Approximate top of of Vanuxem 92 Clinton group 675 Bottom of well at 1792 Clinton group 83 Gas was found at 380 feet in the blue Niagara limestone and continued to about 500 feet. At 685 feet a pocket of gas was developed in the Clinton which was soon exhausted. The gas, when lighted, supports a flame three or four feet high. Wolcott Drilled October 1887 Altitude approximately 317 ft A. T. 3 Red shale with red 1 Shaly layers of Niagara limestone above aud alternating siliceous Clinton below 214 feet sandstone forming the 7 2 Oolitic iron ore and red Medina 690 feet Shales of Clinton 4 Oswego sandstone of group 16 Vanuxem 210 aC. E. Ashburner. Petroleum and natural gas in New York. oC. 8. Prosser, American geologist. Oct. 1890, p. 203. 1888, p. 36. 28 | NEW YORK STATER MUSEUM 5 Some blue shale alter- 8 Lower part of Utica nating with gray sili- shale 590 feet ceous sandstone simi- 9 Compact blue limestone lar to the Oswego alternating with shaly sandstone 170 feet layers forming top of 6 Undoubted Hudson riy-- the Trenton 750: er blue shale 15 7 Gray sandstone contain- ing gas, followed by dark blue shale 3 Gas was found from 1100 feet on. The largest amount came from the sandstone at 1355 feet in the Hudson river group. Veins were also found in the Trenton limestone at 2092 and at 2330 feet, the larger quantity at the greater depth. The well gave a metered flow of 5000 cubic feet of gas a day. Wells in Monroe county Rochester Record by Prof. H. L. Fairchild@ Altitude 484 feet A. T. Drift 22 feet Trenton 954 feet Niagara and Clinton 228 Calciferous (?) 137 Red Medina 1075 Archean 3. Oswego or Oneida 83 . Bottom of well at 3100 Hudson river and Utica 598 No gas of consequence. Brockport Record by Prof. C. S. Prosser@ Altitude 538’ A. T. Depth 500 Medina red shale 900 Darker red shale 950 Very dark red shale 1000 Gray and bluish chips. ) Medina About 4 are light gray, a. ign ous oe calcareous Loe a -a's slightly | SHO 1400 Blue shale and sandstone} H™ - @ 2000 Blue compact Trenton limestone to bottom of well. A small flow of gas at 1200 feet. a@ Proc. Roch. acad. sci. 2:91. PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 29 Wells in Niagara county Gasport The following record is furnished me by Prof. C. S. Prosser who obtained the data from Mr C. V. Mesler of Gasport. ( Loam 8 feet to Skeet Shale 6 feet to 14 i Clinton sandstone (7?) 8 feet to 2 = Medina sandstone 50 feet to 72 a ‘ Marl 8 feet to _ 80 a | Gray belt 24 feet to | 104 Medina marl or shale of the Medina epoch 716 feet to 8204 | Argillaceous sandstone 60 feet to 880 me f Blue alternating with red shale 280 feet to 1160 feet S| Gas at 1080 EE ‘ Blue shaly limestone of the Hudson riv. epoch 340 feet to 1500 a | Dark, slaty bituminous shale of the Utica epoch 300 feet to 1800 = (,Trenton limestone 170 feet to 1970 feet a d Chazy limestone of Trenton epoch 30 feet to bottom of well E | at 2000 Holly Bored 1897-98 Record by J. W. Stearns, contractor Red Medina sandstone Black shale 850 to 1420 feet and shales mixed to 600 feet ‘Trentonlimestone 1420 to 2025 Oswego sandstone 600 to 850 when drilling was stopped. Small flow of gas at 1770 feet Best gas at 1965 feet More gas 1827 Big pocket of gas 1975 Mr Stearns reports a confined rock pressure of about 200 pounds, and estimates the production at about 100,000 cubic feet a day. Lockport About two years ago a well was sunk on the farm of J. Wright McCollum in what is known as the “ lower town.” The mouth of the well is at about the horizon of the Clinton limestone. At a depth of about 1150 feet a small vein of gas was found which gave a confined rock pressure of 87 pounds after 24 hours. The well was drilled to the middle of the Trenton limestone with- a The upper 187 ft marked ‘salt.’ 30 NEW YORK STATE MUSEUM out finding further gas and was abandoned at 2150 feet. The gas was piped to Mr McCollum’s house and now supplies five stove and grate connections, and 30 gas burners. The gas is said to be of a quality fully equal to the illuminating gas furnished the city of Lockport. ; Clifford Bros. are now sinking a well for gas near the canal opposite the Erie railroad station. It is intended to proceed no lower than the white Medina sandstone. Record of well no. 2 of the Niagara oil and gas co. Located on the Bradshaw farm near Coomer p. o., dist. 13, lot 36, township of Newfane® Drilled Jan. 4, 1892 Red Medina, dark Hud- Calciferous 1910 to 1980 feet son river and Utica Hydromica and dark shale to 1200 feet green schists of the Trenton 1200 to 1910 Archean 1930 to 1980 No Potsdam The well had a little gas from 1912 to 1918 feet. Well was cased to 248 feet and was dry afterward. CONCLUSIONS REGARDING NATURAL GAS IN THE DISTRICT STUDIED Careful observations extending over Erie co. and eastward as far as this investigation has gone, lead me to the following con- clusions regarding natural gas: 1 It originates from the decomposition of organic matter, and accumulates in the same or an adjacent overlying stratum which acts as a reservoir. 2 This reservoir-stratum may have an impervious cap which prevents the upward movement of the gas: or it may be porous like sandstone, or contain wide joints or fissures like limestone. 3 The capacity of the reservoir depends upon the thickness of the stratum; the looseness of cohesion among the grains compos- ing the sandstone, or the size of the joints of a limestone; or the form of structure which the reservoir takes, as for example an anticline or arch. a See report of N. Y. state geologist. 1895, p. 386. PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK aa 4 Where the rock dips uniformly in one direction, as it does in western New York, the gas has a tendency to escape at the northern outcrop. Consequently small quantities of surface gas may occur at the reservoir outcrops, and borings near these outcrops will find very little gas or gas at low pressure. 5 In general, deep wells show greater pressure than shallow ones; and this is, in many cases at least, independent of hydro- static causes. 6 The gas-horizons in the district under consideration are the Trenton limestone, the Medina sandstones, the Clinton, the Nia- gara limestone, the waterlime beneath the Corniferous lime- stone, and the Marcellus at about the horizon of the Stafford limestone. Shallow wells have found an inconsiderable amount of gas among, or just below, the Portage sandstones. 7 South of the Corniferous outcrop, borings extending into and through the Trenton have not found paying gas in the latter formation. North of the Corniferous outcrop the yield in the Trenton has been better, but can not be considered as paying. These borings have been so expensive and unsatisfactory that further attempts to reach Trenton gas are not recommended. 8 The Medina sandstone is the best producing rock, and nearly all the gas is found within 200 feet of the top of that formation. In Erie co. the Quartzose sandstone of Hall, or “* White Medina ” as it is generally called, is the main reservoir. It is less than 150 feet below the top of the Medina and thins rapidly eastward from Erie co. ‘ 9 The presence of gas in the Quartzose sandstone appears to depend upon the softness of the rock. If anticlines in the stratuin occur, they are too low to be perceived. 10 The Clinton has furnished paying gas in a few instances. 1i A small quantity of gas containing sulfureted hydrogen is often found in the upper part of the Niagara limestone. This does not pay except where used with gas from a lower level. 12 The honeycombed waterlime beneath the Corniferous often contains pockets of gas, and in the case of the Kelly well at Zoar has given the best well in Erie co. It is a promising ‘horizon where wells are started on the Portage outcrop. 54 NEW YORK STATE MUSEUM 13 Borings along the Medina outcrop and the northern edge of the Niagara have been unprofitable. | 14 A number of wells drilled along the northern edge a the Corniferous outcrop and in one case (at Getzville, N. Y.) on the Salina outcrop have yielded a fair amount of gas. 15 The greater part of the paying wells are located along the Marcellus and Hamilton outcrops. PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 33 OIL AND NATURAL GAS IN CATTARAUGUS CO. Historical The development of the petroleum industry in Cattaraugus co. began near the village of Limestone in 1864. The first well in the Tuna valley was drilled by Olmstead on the Crookes farm in Pennsylvania, about one half mile south of the state line. The discovery of a small amount of oil in this boring stimulated exploration, and in the early part of 1864 Dr James Nichols, Henry Renner and Daniel Smith sunk a well just north of Lime- stone village, to the depth of 570 feet. They found oil, but not in paying quantities, because as was afterwards ascertained, they did not go deep enough. Soon after, the Hall farm petroleum co. of which Job Moses was a prominent member, put down a well about three fourths of a mile west of Limestone on the opposite side of the valley. Oil was found in the third sand at a depth of 1060 feet and yielded for a few hours at the rate of 200 barrels a day. Owing to an accident, the well was ruined by an influx of water before its true value was ascertained. Moses immediately purchased 9000 acres in addition to the origi- nal tract of 1200 acres, and leased 1000 acres more. The further development of the property appears to have lan- guished and the operations of Moses were unprofitable. In the same year Dr Nichols and others sunk an unsuccessful well on the Bailliet farm, north of Limestone. The oil excitement of 1875-76 caused a rapid development of territory along the Tuna valley. The first productive wells were drilled on the farms of Hiram and William Beardsley. These found oil in paying quantities and in a few months the valley was dotted with derricks. In the fall of 1878 there were more than 250 wells in Carrollton township alone. Explorations northward began in 1876, when the Allegany oil co. put down a well on the premises of J. G. and E. M. John- son in Allegany township. Oil in paying quantities was obtained, and rapid development followed. The discovery of oil in the Woodmancy well near Allegany village in 1878-79 opened up a 34 NEW YORK STATE MUSEUM new pool which was still further developed 10 years later. The wells here are small producers and appear to mark the northern limit of oil territory in the county. | Pipe-lines® 9 In 1873 J. H. Dilks organized the Olean petroleum co., estab- lishing headquarters at Olean. The construction of a pipe-line to New York was immediately begun, and on Thanksgiving day of that year the first oil was pumped through a section of pipe 144 miles in length. In 1876 this company was succeeded by the Empire transportation co. In 1879 the United pipe-line, afterwards the National transit co., bought the stock and inter- ests of the Empire co. and began the erection of storage tanks. At one time there were in the vicinity of Olean 300 tanks hav- ing a capacity of 9,000,000 barrels. From Olean as an initial station, two six-inch lines now extend to the seaboard through which 35,000 barrels of oil can be delivered each day. Refining In 1877 a refinery of two small stills was erected by Mr East- man on the site now occupied by the Acme works. This soon passed into the hands of Wing, Wilbor & Co., who added a 500 barrel still. In the following year the property was purchased by the Acme oil co. of Titusville, Pa., which immediately began the enlargement of the works. At the close of 1885 the number of stills had increased to 25, with boilers, tankage and other acces- sories in proportion. In 1894 an additional plant was erected to refine the Ohio crude oil. The plant now owns 49 stills and 153 tanks and refines 5000 barrels of oil a day. Explorations for gas and oil In the northern half of the county several borings have been made for gas and oil, none of which have been commercially prof- itable. Inthe greater number of instances either no records have been kept; or if kept, are too incomplete and inaccurate to be of much value. The well drillers, usually imported from the oil EEN INI DS ARTS a Information from W. M. Irish, gen. mgr. Acme works, Olean, N. Y. PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 35 regions of Pennsylvania, have disregarded everything except sandstones, in which they had been accustomed to find oil or gas, and so valuable stratigraphic information has been lost. In a few instances owners of the wells have been disposed to withhold information, specially if the well was a “ wildcat” in a hitherto unexplored district. This inability to procure accu- rate information has left gaps in our knowledge which make the task of correlating the strata already recognized in Erie co. with those occurring in wells farther south exceedingly difficult. The records which follow are believed to be accurate within the limits claimed. a Gowanda wells At Gowanda two wells have been sunk on the Cattaraugus co. side of the Cattaraugus creek. The following original record of the old Vinton well kept by the driller, Mr J. D. Rickerson, differs slightly from the one already published.@ Vinton well Completed Mar. 23, 1883 Salt water at 250 feet Top of Corniferous lime- Gas and oil 458 stone at 1580 feet Oil 904 Water 1580 Gas 1006 Well finished in water 1700 Cased to 100 feet. This record places the horizon of the Corniferous limestone at 1580 feet, 290 feet deeper than in the record furnished by Mr Vinton. In July 1897 a well was put down on the Ross farm two and one half miles east of Gowanda near the junction of the two branches of Cattaraugus creek. The following record was fur- nished by Mr Charles Howland who was on the spot while the well was being drilled and who kept careful records of the depths. Gas at 246,570,598 and 1193 feet Green oil at 1707 feet Corniferous limestone at 1505 More green oil 1765 Amber oil 1626 Bottom of well 2060 a See author’s paper, 5th an. report of N. Y. state geologist, 1885. 36 NEW YORK STATE MUSEUM The well was shot at 1626 and 1710 feet producing a heavy oil having the color of new cider. At the time of my visit in August 1897, the well was reported to contain 100 feet of oil resting upon 900 feet of water. Mr Howland thinks the well would have yielded better if shot at 1765 feet. As it has not been pumped, the daily yield has not been ascertained. | In the Zoar gas field on Cattaraugus creek, six miles south of Springville, a well? on the Cattaraugus co. side passed through Drift 80 feet Show of oil and gas at 1865 feet Top of Corniferous lime- Depth of well 1950 stone at 1700 The well has no gas worth piping. The Kelly well across the creek in Erie co. found.” Corniferous limestone at 1500 feet Amber. oil and = “salt Green oil and gas 1725 water at 1760 feet The two Gowanda wells and the Zoar wells quoted above are the only borings in the northern part of the county where a fair showing of oil has been found. The amount thus far discovered is, however, insufficient to warrant the belief that oil exists here in paying quantities. The data furnished by these well records, which are believed to be as reliable as can be obtained by the ordinary methods of drill- ing and measuring, show the horizon of the top of the Corniferous limestone to lie at Gowanda about 1500 feet below the surface. The top of the corniferous at Buffalo creek is approximately 573 feet above tide. The elevation of Gowanda station is 772 feet. Assuming the air line distance between these points as 27 miles, the average dip of the top of the Corniferous is hee 48 feet to the mile. Wells have also been put down at Snyder’s schoolhouse, lot 50, town 5, range 8, and at Smith’s Mills nine miles west of Gowanda. No record of these has been preserved beyond the fact that the first was about 1000 feet deep. a See author’s paper, 16th an. report of state geologist, 1896. PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 37 The Alder-bottom well This well was located on lot 22, range 9, township of Leon about six miles west of Cattaraugus village. Mr J. W. Stearns -who drilled the well informs me that the drill encountered noth- ing but shales till the Corniferous limestone was reached at 2255 feet. Drilling was stopped in the Niagara shales, as he believes, ' at a depth of 3000 feet. Other borings In December 1897 a well was sunk at East Otto by Mr Arthur Richardson. The well is reported to have stopped in water at 2753 feet. No record has been obtained. At West Valley on the Buttalo, Rochester and Pittsburg rail- road a well was sunk for gas several years ago without success. No record has been preserved. In the vicinity of Ellicottville four wells have been drilled, all of which have proved barren. Three of these are located in what is known as the Somerville valley, two miles east of the village. Well no. 1 of this group gave, according to Mr Hickey, the contractor, the following approximate record. First sand, with a little 30 feet of black shale gas at about 250 feet with some oil at 1340 feet Second sand 725 Sand 1600 Third sand 1050 13 feet of shells 1790 Bottom of well 1803 The well furnished very little gas. Well no. 2, one mile east of no. 1, found 35 feet of sand having a show of oil at 475 feet. Drilling to 1809 feet disclosed no fur- ther oil or gas. A fourth well was put down in the latter part of 1897, three fourths mile west of the village without finding gas. This well was 1651 feet deep. Four wells have been drilled in the vicinity of Franklinville, one of which was 2500 feet deep. The Simonds well 2400 feet in depth gave a small amount of gas, but not enough to be of commercial value. Of the Ogilvie well located east of Franklin- ville no information was obtainable. All these wells were prac- tically barren. 38 NEW YORK STATE MUSEUM In the townships of Conewango and Randolph several borings have been made, the records of which are meager and unsatis- factory. The well drilled at Conewango in 1865 is reported to have been 840 feet deep and “dry.” ‘In the vicinity of Ran- dolph five borings are reported. One on the Albert Gasman farm in Randolph village is said to have passed through a white peb- ble sand containing some oil. Gas from this well was piped to . Mr Gasman’s house and supplied it with fuel for two or three years. The gas horizon is given as 800 feet. Another well sunk for water near the Chamberlain institute failed to reach the bottom of the drift at 400 feet. Two wells are located at East Randolph and two on the Scud- der farm one mile southeast of Randolph. No records of these could be obtained. Mud creek field A group of four wells is located on the county line, partly in Chautauqua co. and partly in the southwest part of the town of Randolph. One well was drilled 36 years ago, the others in 1896-97. The following record was furnished by Mr J. E. Hazard of Randolph. | | Well on Walker farm, s.w. part of Randolph township Rock at 30 feet Oil sand 23 feet at 830 feet Shale and sand to 170 Gas in shale 400 A little gas in sand and Sand (40 feet) (Dewdrop?) 490 shale at 170 Best gas 502 Gas estimated to be 50,000 feet a day. Another well just on the Chautauqua co. side of the line is said to furnish 100,000 feet a day. Mr John W. Knox reports the rock at Mud creek to dip to the east. Several borings have been made near Little Valley of which no record has been kept. One was located two miles west of the village and was barren. The well on the A. B. Chase farm was drilled to 1400 feet and is said to have yielded, at one time,’ a strong flow of gas. Another well on the Winship farm was drilled to the depth of 2000 feet but proved to be entirely barren. PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 39 Little Valley township A boring which at one time gave promise of a remunerative supply of gas was located on the farm of Mr John E. Leach about one and one half miles northeast of Elkdale station. Samples of the drillings were shown me by Mr Leach from which the fol- lowing notes were taken: Sandstone 130 to 140 feet Blue gray shale 1160 feet Sandstone 200 to 240 _ Blue’ gray shale : IZ Calecareous sandstone 300 Harder blue gray shale 1290 Calecareous sandstone 350 Shale 1450 Argillaceous sandstone 600 Black shale 1488 Hard argillaceous sand- Biue shale 1530 stone 620 Black shale 1590 Pocket of gas in hard Gray sand with some argillaceous sandstone 630 oil 1740 Hard argillaceous sand- Gas which wasdrowned stone 850 out by salt water 1980 Softer argillaceous sand- stone 884 Sufficient gas was obtained from the lower level to furnish four stoves for a year. The pocket found at 630 feet gave a large flow for 16 hours and then ceased almost entirely. Salamanca township A well on the Rich farm, lot 18, township of Salamanea is said . to have furnished a small flow of gas. No record has been pre- ° served. Wells on both sides of the valley below Salamanca have proved entirely barren. The following record shows the conditions found in this vicin- ity. | Salamanca centennial well, Oct. 28, 1876 @ Record by H. A. Darrow Well mouth A. T. 1554 feet Conductor 9 feet Gray slate and shells 441 to 450 feet Gray slate with First s. s. 450 455 Shells 784 to 1120 feet Gray slate 455 750 DhIiTd WSS 1120 1138 ? 750 780 Gray slate with Second s. s. 780 38784 hard shells TASS elSsZ5 Cased at 241 feet. A small quantity of gas at 900 feet. Un- remunerative. a Pa. second geol. survey 14, p. 10], 40) NEW YORK STATE MUSEUM Peth well. Near Great Valley, N. Y.— Drilled by O. A. Knox, Bradford, Pa. Record from R. EF. Gilman, Great Valley Drive pipe 66 feet Gas and 20 ft sand at, 650 feet Gray sand, 6 ft at 430 Slate to 1570 Dark sand, 15 “ 470 Sand, 30 ft with no Slate and shells, 40 ft gas at 1570 A little gas at 570. ; Completed at 1650 feet. This well furnished a small but permanent flow of gas which has not been utilized. ; Two wells producing a small quantity of gas are located on the land of Mr Ostrander at Killbuck. They are not commercially profitable. | : The Humphrey field During the year 1897 nine wells were put down in the south- west part of the town of Humphrey, in four of which some oil was found. The successful wells are located on lots 50, 51 and 59, and on Mar. 1, 1898 were producing altogether about 10 barrels of oil a day. At that time a total of 400 barrels had been run into the pipe-line. Record of well no. 1, Hd. Guthrie farm, on lot 51, Humphrey, be- longing to the Union oil and gas co. Sunk in May 1897 Record from B. C. McIntyre 8 inch drive pipe Top third sand | at 1236 feet through gravel and Sand and shells 1286to 1272 quicksand 85 feet Oil, and gas enough 12 ft white sand with for boiler at 1272 a little oil and gas Chocolate (Bradford?) at 310 sand 1272 to 1800 First regular sand, Sand and shale mixed, STAY. 2 mit ee tele with 12 ft of black with a little oil and Shale full of oil at salt water at. b10 the base, to the bot- Top second sand 1035 tom of well 1372 The bed-rock first reached by the drill was a white, flat-pebble conglomerate. a A test well was bored in Humphrey about the year 1878 by Golden, Fowler & Humphrey. The well was 1500 feet deep and barren. PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 41 Well on the Childs farm, belonging to Union oil and gas co. Record from B. C. McIntyre: Mouth of well approximately 1500 feet A. T. To bed-rock, a soft con- Oil and gas in choco- glomerate 15 feet late colored sand First gray sand, 20 ft at 580 (Bradford?) .12 ft No second sand | thick to 1357 feet Top third sand at 1805 Total depth, finishing Shells and sand 1805 to 13845 in shale 1403 Bear Hollow well, belonging to the Orchard park oil and gas co. Record from B. C. Mcintyre Elevation of mouth of well approximately 1800 feet A. T. Bed-rock at 20 feet Bottom of Bradford Cased to 220 sand at 1488 feet Top of Bradford sand at 1417 Black (McKean?) sand, 30 ft 1618 The Bradford sand yielded gas and about a barrel of oil a day. Three additional wells were drilled Mar. 1, 1898. Well at Ischua Record from E. J. Fish by C. E. Banfield This well is located three quarters of a mile east of the village in the s. e. corner of lot 8, Ischua township. First sand containing Light colored shales a small amount of with some shells 750 to 1150 feet black heavy oil and Black shale from 1150 1725 a little gas from 140 to 160 feet Coarse red sand with- Shells with a little gas at 750 out gas or oil 1765 Total depth ; 1802 Well unproductive. Hwunsdale A well put down about 20 years ago on lot 48 near Hinsdale village is reported to have given a small showing of oil. Another on lot 12 was entirely dry. Five years later a well was bored near the Western New York and Pennsylvania depot which gave a large flow of gas for several years but has now ceased to pro- duce. This well was 1200 feet deep. Another, one mile south % 42 NEW YORK STATH MUSHUM of this, struck a small flow.of gas at-1200 to 1300 feet below the surface. During the summer of 1896 a well was bored on the edge of Hinsdale township near the county line, not far from Cuba. Neither gas nor oil was found. 8 About 32 years ago a well was put down by Mr T. P. Snyder on the old Indian reservation near Cuba in Allegany co. Mr Snyder reports a small showing of gas and heavy oil at about 370 feet. As the well was drilled wet and not properly cased, its possibil- ities were never ascertained. Well no. 2 drilled by Mr Keeney gave some gas but no oil. Southern tier of townships All the townships bordering upon the Pennsylvania line have furnished small amounts of both gas and petroleum. The terri- tory in which these products occur in commercial quantities is limited almost entirely to the townships of Carrollton and Al- legany, which have produced more than nine tenths of all the oil thus far marketed from the whole county. A small oil field also occurs in the southern part of Olean town- ship and a few productive oil wells have been recently found in Red House. . . | South Valley township Near Onoville two wells have been sunk to the third sand at a depth of 1200 or 1500 feet. One of these was barren; the other gave gas which, if used, would supply three or four families. A third well was in process of drilling in April 1898. Red House The discovery of gas in the Red House field was first made in February 1891, the principal horizon being the second sand. The original confined rock pressure in the best wells was 225 pounds, which had, in August 1897, fallen to 100 or 125 pounds. My informant, Mr E. W. Lewis of Bradford, estimated the total output of the Red House field at that time to be 30,000,000 cubic feet a month. PETROLEUM AND NATURAI: GAS IN WESTERN NEW YORK 43 A small portion comes from the Rice Brook field, but the greater part is furnished by seven wells in the eastern part of the town. One or two wells on lot 44 supply about 210,000 cubic feet a day additional to the Smith chemical co. of Brad- ford. The gas from Red House and Rice Brook also supplies the villages of Limestone, State Line, Carrollton and West Branch. In addition to 376 stove connections, it furnishes fuel for the two large boilers at the Limestone tannery, for the power house of the Olean, Rock City and Bradford electric railway at Red ‘Rock, for four oil well boilers and for the 24 retorts of the Chemical works at West Branch. A well with an estimated flow of 9,000,000 feet of gas a day was completed in April 1898, in Pennsylvania, just south of lot 1, in the extreme southeast part of this township. No borings have been made in Red House to ascertain whether the pool ex- tends into this state. Well records Information from Mr Miner Wellman, Friendship, N. Y. Messrs Doherty, Wellman and Corbin have producing gas wells on lots 6, 18, and 14 Red House township. The well on the west part of lot 18 had an original rock pressure of 227 pounds and a measured volume of 1,000,000 cubic feet a day. Another southeast of the middle of lot 14 had an original rock pressure of 200 pounds with a measured volume of 9,200,000 cubic feet a day. ~ ! Harbel well, no. 1 24 feet Third sand 286 Full depth at 1315 Torpedoed Drilled out and shot again at 1325 to 1355 feet. 1332 feet at 1305 1365 feet at 1311 1335 feet 1385 at 1370 Well no. 3, John Zaph farm, same lot, Allegany township Conductor Casing Sand at _ Casing Sand Conductor Casing Conductor Casing Top sand 30 feet Total depth 179 Torpedoed at 1415 | aro tla John Frieze well, lot 1 Drilled October 1878 268 feet at 1300 Bottom of well Frieze well, no. 4, 1879 10 feet Bradford sand 372 Total depth Joseph Falkel well, no. 2, lot 1 36 feet Bottom sand 292 Total depth 1420 1473 1427-36 feet 1420 feet 1040 feet 1602 143914 feet 1505 58 NEW YORK STATE MUSEUM Wells in this field started off at about 50 to 75 barrels or better, one giving as high as 300 barrels. The production usually drops to 15 or 20 barrels in from three to six months. | Olean Borings for oil in this township have discovered but one im- portant pool, that known as the Meek’s creek or “ Haymaker ” field, located on lots 3 and 4 of section 1, and lots 1 and 2 of section 5, in the southern part. This group embraces about 200 wells from 1150 to 1170 feet deep, getting oil from the Bradford sand. | The best wells in this pool gave, on the start, as high as 75 barrels a day, but at present the production has fallen to one barrel a day, or less. The greater number which are still pumped fall below a daily yield of one half barrel. Just southwest of Olean city on lots 8 and 10, is a small pool where three wells yield about a barrel each of oil a day. Bor- ings in the northeast corner of the township have found the edge of the Allegany field, but no producing sands of consequence. A number have given a show of oil in the Allegany sand, but not sufficient to pay for working. About 30 barren wells are reported in the townships east of Olean city. Four of these are located on lots 1, 2, 6 and 7 of section 4. _ A little gas was met in two of these, but not enough to be utilized. The well records which follow were accurately kept and are believed to be reliable. Record of well no. 1, section 6, Olean township. Belonging to the Devoman oil co. Authority, W. M. Kincaid Casing 244 feet Top third sand (shells) at 1890 feet Top Chipmunk sand at 850 Bottom of third sand Bottom Chipmunk sand 880 (shells) 1451 Top second sand 990 Bottom of well 1714 Bottom second sand 1051 PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK oD The first sand had some oil and gas, and a trace of oil also oc- curred in the chocolate-colored second sand. From 1007 to 1014 and at 1032 were streaks of gas, the latter burning as high as the walking beam. Well no. 1, Downing farm, lot 1, range 1, Olean township . Casing Gas sand Oil Gas sand Oil Casing Gas sand Oil sand Casing Gas sand Oil sand Authority, Franchot Bros., Olean. 470 feet Bottom of oil sand at 1700 feet at 1620 Bottom of well 1749 1675 Olean township, Downing no. 3 at 1420 feet Bottom of oil sand at 1506 feet 1473 Depth 1530 Downing no. 17 300 feet Bottom oil sand at 1281 feet at 1213 Depth of well 1326 1251 Downing, no. 2 | 510 feet Bottom of oil sand at 1668 feet at 1593 Bottom of well 1691 1648 Torpedoed 1628 to 1626 McMullen and Hallock gas well 4 May 23, 1877 Located on the Loup farm, section 1, extreme s.w. cor. Olean 675 to 890 feet township Well mouth A. T. 1785 feet Gray slate with Conductor 16 shells Cased to 196 Second sandstone Gray shales and slate with thin sandstones to 625 First sandstone 625 to 675 890 to 960 (?) with sandstones 960 to 1155 Sandstone withgas 1155 to 1180 Slate 1180 to 1187 (?) 1187 to 1120 - Third sand with slight show of oil 1220 to 1240. aC. E. Ashburner, Petroleum and natural gas in New York, 1888, p. 34. 60 NEW YORK STATBH MUSEUM A month after drilling C. A. Ashburner estimated the flow of gas from this well at 24,480,000 cubic feet a day. The life of the well was brief. In 1888 the well produced from two to three barrels of oil a day. The Bradford oil and gas sand was struck at a depth of 1230 feet, or 1785 feet below the bottom of the Olean Conglomerate.® PORTVILLE South and east of Hinsdale village and for the most part in — Portville township, about 20 borings are reported, in no one of ~which gas or oil was found in paying quantities. The following ‘reliable record furnished by Franchot Bros., Olean, shows the geo- logical conditions existing in one well. | Mitchell well, no. 1, lot 36, range 2, Portville township ‘Drift 60 feet Sand, 20 ft. thick, Fresh water to 272 with gas at 985 feet Salt water DAG Top third sand 1060 Stray (?) white pebble Bottom third sand, gas sand * A0ie4ftr thick and show of oil 1085 with heavy oil at 384 Fourth sand 1214 to 1272 Regular first sand, 20 Shale and sand to 1513 ft with gas 743 Limestone shale and Regular second sand, sand | 1513 to 15387 20 ft with gas 930 Mixture of limestone, shale and sand 17521%4 A heavy pocket of gas was found in a sand at 400 to 420 feet. In a well on lot 18, s.w. corner of Portville township, accord- ing to Mr E. J. Fish, a shell containing some gas was found at . about 600 feet. At 972 feet a gray sand 38 feet thick was pierced which pro- duced about half a barrel of oil a day, and gas enough for a dozen families, if it had been utilized. A third sand two feet thick with no oil or gas occurred at 1125 feet. Two wells have also been sunk by Mr Comstock of Portville, one just north and the other just south of the boundary line be- tween lots 14 and 15. The well on lot 14 had a small flow of gas b Pa. second geol. surv. 14, p. 99. PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 61 at about 1000 feet and a show of oil at 1500 feet. Both wells. were valueless. | Mr E. J. Fish reports a well on lot 50, in which a sand 22 feet thick, producing half a barrel of oil a day was found at 960. feet. The well was continued through black shale to 1110 feet and abandoned. Wells on lots 10 and 11 have produced small quantities of oil: and gas, but not enough to be commercially profitable. Barren. wells are also reported on lots 1, 16 and 35. Production of petroleum in New York state The following summary furnished by Mr John O’Brien, sup’t of the National transit co., shows the amount of oil handled by the pipe-lines from Jan. 1, 1897 to Aug. 1, 1898. Statement of oil produced in New York state from Jan. 1, 1897, to Aug. 1, 1898. 1897 Allegany co. Cattaraugus Co. Total 2 EES ene 57,004 69 69,437 84 126,972 53 PEPE iano 0.5, Si5\< ai oye dissseume. ne opis 59,681 89 69,798 11 129,480 00 WON AA eeetcie os 6) 05,16 16) Sais. apis 0, deine 63,720 97 84,195 88 147,916 85 2 LET age alee inal eerie late palpi earners 62,955 54 79,127 36 142,082 90 DEY A eee aka eter saeels a ee Gout atte e's 63,076 51 83,4738 08 146,549 59 miner AT! . O06 i. 23 RSI aLOn 62,651 55 84,848 56 147,500 11 PaaS oe Gace sh 5: ofeNS [ol dial a oj iste usa 62,525 21 84,492 05 147,017 26 RAMUMED ME Marat oc ohalsyase' a icalcpasciisy ae | | a es | [ Gi Saal = s tal in | | | | = = aR Py a 3 5 a | # Ss — 3 | =f = = i SB oa | ape pigs 7 3 Ue Pe ee by Scale, 1M inches «2miles OIL MAP! Oi hire: CATTARAUGUS OIL AND ons FEE GANS) ONS WRG) IP N.Y. ’ CATTARAUGUS COUNTY 1898 Ane oe ota GADD ee SA ence a ee Pod day ine: PETROLEUM AND NATURAL GAS IN WESTERN NEW YORK 63 Map The accompanying map shows the present extent of the oil- pools of Cattaraugus co. in which the product has been found in commercial quantities. In the case of the Chipmunk pool the same oil-producing sands will undoubtedly be found, in the future, to extend much beyond the southern and eastern limits laid down upon the map, and may be found to include a part, at least, of the Rice Brook field. It has been my purpose however to avoid speculation and to include only such facts as are known to date. I wish to acknowledge my indebtedness to Mr John Greenwood of Limestone, N. Y., whose intimate knowledge of the oil in- dustry and of oil territory has been freely placed at my disposal while constructing the accompanying map. Respectfully submitted Irvine P. BisHoP CLASSIFICATION AND DISTRIBUTION. OF THE HAMILTON AND CHEMUNG SERIES OF CENTRAL AND EASTERN NEW YORK PART 2 CHARLES S. Prosser COWEN S aT ROCWCHON Fee Oe Pas ee ice eeu eh se gee cha, Sh anne 2 Ome Susquehanna valley Scibn wbinlesaverelle 6 Ute uheras whdeie Wc cette ist ian 67 OVMOON UA Iie ars «aoe she Ploie ow O's ele one lwo oi Gove take tale 68 WVieSEIOMCO NTA. ces ie ahaa oo. re rr 85 MO Une ne woie pe iota vole anche setae Veplinndield aa e 8 ke 86 AG amen ES NG Sis Cig e oinilone wf Wee he ene a oleae er 91 MTHS Oy oh esa deoe Hwee we os) by, dlieiv be Sd ole ovens rr 94 JANGET ES DSN I ORL gs ERNE IBIAS Cac ‘othe ee Gea 98. DOTA ATE ICOUTILY Wei ee os Gio bayele’a ta ie o caaee Sih 105 MSO VIMe i oie. oie ood Sickel wale ws wielecn gh ole) Shem: an 105 ERIM chess eich a fal leat ea sn. feo, stele sit/2 necel@t 4 ke er 106% PMc TTI ia tee doin loo Gud tA: aiydiatve ales le Si cn er dais Melaware valley. is foe dois coins dice ee 122 PUM UINGWS LE erie oh sel a eae win ov soe ae lee ie ini neu chs os) se er 134. Gliaelotie valley S@CtiONs 75 iis elec. ack s oaje' d ahane! ds lees 138 Aye UUM Ge sk Eos dln ig alae a dooce ee ote ial ane seid aoe a ee 138 WHOUCESLER ey nc ie by oe ee ake en OU. 141 OU! LESTE Pete i Ra is Se Eg Ce Per PUG AM gE ape 151 BESO Ce PLC Sw Masia a sda hes oe eo ly tc anal tree 6 160 Schoharie valley section... 6.2...:0... ‘sa ala cla es ee 163 UES Se i is ail aides he Ries. ose ene ee er 166 COT Gites e's end sek whe oe ohn a WG : BLM se a a © a ate ap le Wie Sule ala! wwe Wa ohe We 0 oer 194 COE AIO CT Jig ANGST A ERR AE it Menge OO Pee eo 206 Opmesw med i el. bee a aa Ae 223 POTION pS). 2d (ga ial a oye os bite si sod dnetre Ow Gaye at ae 231 PARAM y COUNTY 63 ke ea ale OD kh 239 Mee Ee eee A eye Ee a tin eas & asters ha aciaes pels a saudi “ea le i ea 240 mensselaerville cv Se be ties Cee alse Cee 251 WVIESTORNO he iiele ele a bra etal s Wislene c the ce, Wh ete aioe er 259 CS OCME WCOMITEV sesso. ah eed sie ele ls bie bios 0 oleic sige 4) al Northern TOWNSHIPS. 05. 6 ola kee Glee oe oe le oe 265 FAS LEMON TOWNSHIDS. 5 0505 4).-. als sche eee eo 2g oo eh one 274 Greene county Catskills... 3. 2 tee a i a as Oe 282 Mrs eT EO UNE, oN ow ve ale Oe yhcesace pek 6 oe Rhee eig cane et Aha a ee eps cte Distribution of the Middle and Upper Devonian.......... 289 Srv and Orange COUNTICS |.) 6... /0 (ibis 22 aie, ee teen 1... 804 Distribution of the Middle and Upper Devonian.......... 304 MOEN IESUGTIS 4. Go cle 5 Ook by eatin wlan eR al oS ook ean OR ii ere ea 312 PANDO TUNER ce a IARI Nai Selig: alee’: a col sts owl's, Boe Sele eh bhate penetra 317 Neel ~ it receives Schenevus creek and the Charlotte river from the east. Then its direction is southwest across the southern part of Otsego co., between Otsego and Delaware counties and across the southeastern part of Chenango co., when it turns nearly south- erly and crosses the eastern part of Broome co. into Pennsyl- yania. The Hamilton and Sherburne formations as exposed along the upper course of this river have already been described.? a P. 82-222. ; 618th an. report N. Y. state geologist, p. 198-204 68 NEW YORK STATE MUSEUM Oneonta Oneonta is one of tha southern townships of Otsego co., to the north of which are the townships of Milford and Laurens, the geology of which was described in part 1 of this report; to the west is Otego township and on the south are the townships of — Franklin and Davenport in Delaware co. The Susquehanna river crosses the southern central part of the township from nearly east to west and is lined by steep hills on both the northern and scuthern sides. The northern line is broken by the Emmons, Oneonta and Otego creeks; but the steep line to the south of the - Susquehanna and Charlotte rivers is unbroken save by small _ brooks. : | The Ithaca formation. In the first part of this report the bluish shales containing a few fossils which occur along the river road about one half mile north of Colliersville in the southern part of Milford township were described. These rocks were referred, with some hesitation, to the Sherburne formation and probably belong ~ near its top. On the high hill to the east of the river and. northeast of South Milford are exposures of the Sherburne sandstones.@ XXIII A2. The next locality studied was a glen, known as Collier’s gulf, less than one mile southwest of Colliersville in the southern part of Milford township. From the railroad level to the base of the lowest rocks exposed in the brook is about 45 feet, succeeding which are 60 feet of shales and thin bluish sandstones below the highway. The rocks contain scarcely any fossils and are referred to the Sherburne formation. XXIII A’. In the glen abovethe highway bridge forsome 40 feet the rocks are shales in which Chonetes and Spirifer mucronatus (Con.) Bill. are common. These shales contain the lower fauna of the Ithaca group as it occurs in the Chenango and Unadilla valleys and this zone is referred to the base of that formation. The complete fauna is: 1 Chonetes scitula Hall (c) frill Os setigera Hall ) (c) 3. Spirifer mucronatus (Con.) Bill. (ce) ai15th an. rep’t N. Y. state geologist. p. 202 a No. ZEA SECTION Ai CULLHAS VILLE THIN BLUISH SANOSTONE WITH ABUNDANT FOSSILS — pereter P77 € SAL PALES , 42 PAATLY COVERED,A’ THIN SAN OSTOW E, AF LT GH PROMINENT SAN OSTONWE, A? WE AFA TOP OF CASCAQE, FOSSILS ASG UNDANT, AF ERS SHALES AND BLUISH SAN OSTOVES AA SHE fP#BURNE GovEFE OD .H! A. ff, LEVEL NORKS, a JSLCI/ON LMMN SSA 5 M/.L£.0F ONEONTA. . | MassiVE GREE NISH-— GRAY COARSE SANOSTONE., BASE oF QNEONTA. LEOGE NEAR BFAOW OF STEEP H/LL SOME WHAT CALCAREOUS, ABUNDANT FOSSILS. OCCASION AL OUTCROPS OF SHALES ITHAGA CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 69 4 Palaeoneilo emarginata (Con.) Hall (rr) 5 Leptodesma rogersi Hall (rr) 6 L. Sp. | Ws (rr) Large specimen. ; 7 Lumuilicardium ornatum Hall (?) (rr) Badly broken. 8 Coleolus tenuicinctum Hall (rr) XXIII At. Near the top of the cascade and higher in the glen are thin sandstones. In a layer of the shales near the top of the highest fall, fossils are more abundant, specially Spirifer mesa- costalis Hall (?) which perhaps should be referred to 8. mucro- natus (Con.) Bill. var. posterus Hall and Clarke. This species is common. The other species found in this zone are Chonetes _setigera Hall which is abundant, and Chonetes scitula Hall which . is very rare. XXIII A>. Above the shales of A‘ near the top of the cascade there are from 15 to 20 feet of sandstones whichmake a prominent sandstone zone, some of the layers being quite coarse grained and fairly thick bedded. In the upper part of the zone Spirifer mesastrialis Hall and Actinopteria boydi (Con.) Hall are common; while Spirifer mesacostalis Hall (?) and Tropidoleptus carinatus (Con.) Hall occur sparingly. 3 XXIII A*. 10 feet higher the rocks change to thinner sandstones and coarse arenaceous shales. A layer in this zone contains large numbers of specimens of Spirifer mesacostalis Hall (?) and Tropidoleptus carinatus (Con.) Hall. The fauna is as follows: 1 Spirifer mesacostalis Hall (?) (a) Some specimens resemble S. mucronatus (Con.) Bill., but most of them agree better with this species. 2 Spirifer mesastrialis Hall (G) 3 Tropidoleptus carinatus (Con.) Hall (a) 4 Chonetes setigera Hall (r) 5 Microdon (Cypricardella) gregarius Hall (?) (rr) Broken and imperfect specimen. XXIII A®. For about 35 feet above the conspicuous layer of fos- sils in zone A® the rocks are partly covered along the glen and 70 : NEW YORK STATE MUSEUM then 15 feet of thin bluish sandstones occur. Some of the layers ee : are very fossiliferous and being strongly calcareous form a Sort | te of firestone. The number of species is small, Spirifer mesastrialis = | Hall being the most abundant forms a large part of the thin ~ te ‘ layers of firestone. This zone very strongly resembles some of be see the calcareous layers near the middle of the Ithaca formation at Ithaca, New York. The top of this zone 225 feet above the level of the railroad is at the head of the glen, above which the rocks are mostly concealed by the soil and drift. The following species _ Be were collected in a few moments: 1 Spirifer mesastrialis Hall (c} i" 2 8S. mesacostalis Hall (?) ee 3 Chonetes setigera Hall | er) See 4 Tropidoleptus carinatus (Con.) Hall (ery eee _ In the search for fossils in the zones of this section but little time was spent and more exhaustive collecting would undoubt- edly increase the number of species for each zone. It is con- sidered, however, that these lists when taken into consideration with the stratigraphy of the southern part of Milford township show conclusively that at least the upper 80 feet of the section belong in the Ithaca formation, while the writer would refer the upper 120 feet to that formation and leave the lower 105 feet in — the Sherburne formation. XXIII B’. Three miles east of Oneonta in the eastern part of Oneonta township is the “old Emmons farm ” now owned by M. L. Swartz. At this locality is a ‘steep hill and the base of the | section is at railroad level about one half mile above Emmons : station. .The highway is some 55 feet above the railroad level and then for 265 feet the rocks forming the steep part of the hill © are largely covered and only an occasional outcrop of shale is visible. Then ledges occur forming a conspicuous terrace along the side of the hill which seems to be its brow when viewed from the highway. One layer is hard and somewhat calcareous con- taining some pebbles and plenty of fossils specially Camarotoechia. These rocks contain the fauna of the Ithaca formation, as will be 4 t=: P oe ——— Ck Cee ee re Pity ane me et ae ihe ee CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES: fal seen from the following list of species obtained as a result of a few minutes’ collecting from near the top of the section: 1 Camarotoechia eximia (Hall) H. & C. (a) A O8 stevensi (Hall) H. & C. (c) 3 Spirifer mesastrialis Hall \ (rr) 4 Chonetes setigera Hall (r) a Of scitula Hall } (rr) 6 Paracyclas lirata (Con.) Hall | (r) 1 Palaeoneilo maxima (Con.) Hall (r) 8 Palaeoneilo cf. muta Hall | (r) 9 Sphenotus cf. contractus Hall (rr) Poorly preserved. 10 Goniophora sp. (rr) 11 Leptodesma rogersi Hall (?) (r) 12 Nucula corbuliformis Hall (?) : (rr) 13 Tentaculites sp. (c) All very poorly preserved. | XXIII Bt. 70 feet higher is the base of a massive, greenish gray coarse grained sandstone forming heavy ledges. On the surface the massive layers tend to separate into thinner ones but at a little distance from the surface these are firmly united forming massive strata. There are also layers which are conspicuously crossbedded. This zone has clearly all the lithologic characters of the massive sandstones of the Oneonta formation and repre- sents its base on this hill. It will be clearly shown later in this report that these sandstones are not found at the same geologic horizon from the Chenango valley to Albany co.; but appear at a lower horizon as the formation is followed eastward. It is probable that the lowest of these heavy greenish gray sandstones as exposed at the various localities along the Susquehanna valley do not all represent exactly the same geologic horizon, but they form an easily recognized dividing line and have been regarded as constituting the base of the Oneonta sandstone in this valley. In fact it is doubtful if any line can be found between the Ithaca | and Oneonta formations that can be followed exactly for a con- siderable distance. The lowest red shales and sandstones which have been used by some writers for the line of division between 42, NEW YORK STATE MUSEUM the Ithaca and Oneonta formations are no more reliable than the massive greenish gray sandstones, for they also appear at lower and lower horizons as the Chemung series is followed eastward. It is evident, however, that in the vicinity of Oneonta, Vanuxem, who named the formation, referred these lowest massive greenish — ag oray sandstones to it, for he mentions their crossbedded structure and gives as an example the ledges near the top of the hill below oe Oneonta,? which is the continuation, down the river, of the zone just described. XXIII Ct. Along the highway that turns up the valley of the - brook to the north of the river road about one and a half miles — northeast of Oneonta are exposures of argiliaceous and very thin_ sandstones. Some of the shales are greatly iron-stained. Toward the top of the hill which is covered by the Oneonta formation the rocks are largely hidden by the drift. The shales of Ct along the highway are quite fossiliferous and belong in the Ithaca forma- tion. The list is:. 1 Spirifer mesastrialis Hall | (eh ALS. mesacostalis Hall (a) 3 N. mucronatus (Con.) Bill. (r= 4 Tropidoleptus carinatus (Con.) Beth (rr) 5 Chonetes scitula Hall (r) 6 Camarotoechia eximia (Hall) H. & C. (c) 7 Cyrtina hamiltonensis Hall | (rr) 8 Leda diversa Hall | (r) 9 Paracyclas lirata (Con.) Hall (rr) 10 Nuecula cf. bellistriata (Con.) Hall i (c) Small and poorly preserved. 11 Palaeoneilo cf. muta Hall (rr) 12 Nuculites cuneiformis Con. (rr) 13 Modiomorpha cf. subalata (Con.) Hall . (rr) var. chemungensis Hall This is a more elongated specimen than any figured and in this respect agrees with other specimens seen in the Ithaca formation in the eastern counties. 14 Goniophora carinata (Con.) Hall (rr) 15 Pleurotomaria sulcomarginata Con. (rr) a Geology of New York. 1842, pt 3, p. 187. AS cat Pp CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 73 __ _ XXIII D*.. To the northwest of Oneonta and north of Chestnut | st. is a high hill known as Powell’s hill, the summit of which is over 500 feet above the level of the Delaware and Hudsonrailroad. Below Chestnut st. at the foot of this hill, about three fourths of a mile west of the center of the city is a stone quarry known as the Anthony White quarry which was formerly worked consider- ably for building stone. The base of the quarry is about 10 feet above. the railroad and its wall was formerly 16 feet high. The rocks containing fossils in abundance consist of bluish sandstones alternating with coarse shales. When the writer visited the quarry for the first time it had not been culled and a fine collection of fossils was secured for Cornell university. Three subsequent _ visits have been made which were not as successful as the first. This was due in part to lack of active quarrying and further to the fact that several geologists had visited the place for the pur- — pose of making collections. As far as I am aware the complete list of fossils collected at the time of my first visit has never been published, but in the summer of 1895 the following species were «collected: 1 Spirifer mesastrialis Hall (r) 2 SN. mucronatus (Con.) Bill. (c) 3 Tropidoleptus carinatus (Con.) Hall (c) 4 Chonetes scitula Hall , (r) dC. setigera Hall (a) 6 C. lepida Hall (?) (r) The shape and number of striae agree with this species. 7 Camarotoechia eximia (Hall) H. & C. (c) 8 Strophalosia cf. truncata (Hall) Beecher (rr) 9 Nucula bellistriata (Con.) Hall var. (a) The specimens have same shape though smaller than this species; but are marked with quite heavy lines of growth. This, however, is shown in fig. 7, pl. 46, Paleontology of N. Y., vy. 5, pt 1, Lamellibranchiata 2. 10 Paracyclas lirata (Con.) Hall (he 11 Palaeoneilo maxima (Con.) Hall (r) 12 Microdon (Cypricardella) tenuistriatus Hall (r) 13 Orthonota parvula Hall (rr) NEW YORK STATH MUSEUM 14 Orthonota undulata Con. 15 Tellinopsis subemarginata (Con.) Hall i (rr) ¥ 16 Modiomorpha mytiloides (Con.) Hall biti | ree : pale: Meo concentrica (Con.) Hall Dee aaa 18 Leptodesma rogersi Hall : RGA 9 i0'.5, 19 Liopteria dekayi Hall (rr) 20 Glyptodesma erectum (Con.) Hall (er) 21 Coleolus tenuicinctum Hall | " (c) 22 Tentaculites attenuatus Hall (?) (yrs i 283 Pleurotomaria sulcomarginata Con. | (c) 24 Microdon (Cypricardella) bellistriata (Con.) Hall e 25 M. (Cypricardella) gregarius Hail 26 Grammysia magna Hall 27 G. nodocostata Hall 28 Cimitaria recurva (Con.) Hall (?) 29 Gomophora carinata (Con.) Hall - 30 Homalonotus dekayi (Green) Emm. 31 Nuculites triqueter Con. | 32 Rhodea pinnata Dn. (?): The majority of the 32 species in the above list occur in the Hamilton formation, but the presence of Spirifer mesastriahs Hall and a few other species shows that this fauna belongs in the Ithaca formation of eastern New York. The geological range of 20 of these species was discussed by the writer a few years ago® and it hardly seems necessary to go over that argument again. The rocks of this zone with some of their fossils were briefly — described by Conrad in 1841, who proposed the name Oneonta: group for the formation.° In his report Conrad named and de- scribed the following species: Nuculites cuneiformis, N. maxima (now Palaeoneilo maxima (Con.) Hall), and Cypricardites carinata (now Goniophora carinata (Con.) Hall), from this formation at Oneonta. This name was proposed two years later than that of the Ithaca group by Prof. Hall and apparently was not con- : sidered in the final reports of the New York survey. Vanuxem- a Am. jour. science, 18938, 46: 227. b 5th an, rep’t paleontology of N. Y. (Assembly doc. no. 150, 1841) p. 31. > CLASSIFICATION, BTC. OF HAMILTON AND CHEMUNG SERIES 75 referred to the formation in several places in his final report, but without mentioning Conrad’s name, and in describing this hill referred the rocks at its base, correctly, to the Ithaca group. He states that the rocks of the Catskill group or Oneonta sandstones of Vanuxem “occupy the highest part of the face of the hill, the base of which is composed of rocks which I [Vanuxem] have supposed to belong to the Ithaca group.”* Again, the term Oneonta as the name for a geological formation was already in use, for Vanuxem in 1840 proposed the name “ Montrose sandstone or sandstone of Oneonta’® for the massive gray and red sand- ‘stones and shales that cover the high ground in the vicinity of Oneonta. Later studies have proved that the rocks in the vicinity of Montrose, Pa., belong in a later formation—the Cats- kill—than the higher sandstones about Oneonta, consequently the name Oneonta sandstone has been retained for this forma- tion. Some years ago the writer called attention to this double. use of Oneonta for a formation name and explained their differ- ence in stratigraphic position’. XXIII Dt. A‘tbove Chestnut st. and about 29 feet above the top of the White quarry are fine, blue argillaceous shales which weather to a greenish color and break into very fine pieces. About 11 feet of these shales were formerly exposed but recent building has greatly obscured the outcrop. These shales are somewhat fossiliferous although but few species were ever collected in this zone. The list is as follows: 1 Tropidoleptus carmatus (Con.) Hall (rr) 2 Spirifer mesastrialis Hall (c) 3 Camarotoechia eximia ee H. & C. (r) 4 Strophalosia sp. (rr) 5 Chonetes sp. (rr) 6 Nucula bellistriata (Con.) Hall var. (c) | 7 Paracyclas lirata (Con.) Hall (rr) 8 Crinoid segments (rr) a Geology of New York. 1812. pt 3, p. 192. 64th an. rep’t third district (assembly document no. 50, 1840) p. 381. c Proc. American ass’n adv. science, 1887. 36: 210. %6 NEW YORK STATE MUSEUM XXIII D®. After about 34 feet of covered rocks an artificial ex- ake posure of greenish argillaceous shales was shown in an excaya-_ » tion for a cellar. These shales are fossiliferous, ‘the following are species having been obtained: ia BRO eae 1 Rhynchonella sp. | ACE . 2 Paracyclas lirata (Con.) Hall g(r hades 3 Nuculites cunetformis Con. (rr) = f x 4 Palaeoneilo maxima (Con.) Hall Meee a 5 Grammysia sp. (rr) 6 Tentaculites sp. (rr). 7 Coleolus sp. (rrp XXIII D’. For 99 feet above the greenish shales of D® the rocks oh are mainly covered; but there are loose, angular slabs of arenace- ous Shales to thin sandstones on the surface that apparently came ~ from this part of the hill. These pieces are somewhat fossilifer- ous, furnishing the following list: 1 Spirifer mesastrialis Hall (rr) 2 Camarotoechia eximia (Hall) H. & C. 7 (r) 3 Paracyclas lirata (Con.) Hall | (rr) 4 Palaeoneilo maxima (Con.) Hall (?) (rr) 5 Nuculites oblongatus Con. (?) | (ery 6 Orthoceras sp. (rr) 7 Tentaculites sp. (rr) 8 Crinoid stems (r) XXIII D’. At an elevation 199 feet above the railroad is an ex: posure of 10 feet of rocks. At the base of the ledge is a sand- stone which splits into thin layers and contains an occasional fossil, as Camarotoechia eximia (Hall) H. & C. (?) and a large lamel- libranch shell. Succeeding the thin sandstones are quite argilla- ceous shales which are also fossiliferous and, above the shales, sandstones more massive than those at the bottom of the ledge. In addition to those mentioned above, the ledge furnished the following species: 1 Tropidoleptus carinatus (Con.) Hall _ (tr) 2 Spirifer sp. (r) i CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES ree 3 Nuculites oblongatus Con. (rr) 4 Palaconeilo sp. | (rr) 5 Tentaculites sp. (rr) 6 A small Gastropod | (rs) XXIII D?®. The slope of the hill is then covered for about 189 feet and overgrown with underbrush when the base of the con- spicuous rocks known as the “Oneonta ledge” is reached at 398 feet above the railroad. This is an interrupted and broken ledge vary- ing in thickness from 10 to 30 feet or more, composed of coarse grained greenish gray sandstone that forms massive layers. Suc- ceeding this is a covered slope of 64 feet when a smaller ledge— D¥” of the section—is reached at an elevation of 492 feet above the railroad. At the base is a stratum of coarse gray sandstone } capped by red sandstone. The summit of the hill is somewhat higher but there are no further outcrops of rocks. The rocks com- posing zones D!° and D® are typical exposures of the Oneonta formation. The base of the formation is undoubtedly considerably lower and concealed by the deposit of drift, for on the Emmons farm about four miles east of Powell hill the base of the Oneonta sandstone is 390 feet above the railroad level and on the south side of the Susquehanna river opposite Oneonta it is about 265 feet above the level of the Oneonta railroad station. 78 492’ 428’ 398’ 209’ 199’ 100’ 66’ 55’ 26’ NEW YORK STATE MUSEUM SECTION OF POWELL HILL WEST OF ONEONTA 64’ 30’ 10’ 907 16’ 10’ XXIII D D*? Red sandstone near top of hill \ D1? Covered | D"* Heavy ledge of greenish gray sandstone “The rocks” Oneonta D*® Covered D*® Bluish sandstone and shales Ithaca D" Mostly covered. Loose specimens with fossils Dé Creenieh shales with fossils D® Covered D* Fine blue shales weathering greenish D2 Covered Chestnut street D? White quarry. Blue sandstone and shale Ithaca D? Covered R. R. level t - CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 179 In estimating the thickness of the rocks in the above section I am indebted to Prof. Henry S. Williams who has kindly loaned me notes made by me some years ago when at work on the U. S. geological survey under his direction. ‘These readings have been compared with those taken during the progress of the field work upon which this report is based, which on account of storms were not as satisfactory as desired. The same acknowledgment should be made in reference to the sections described later, north of Otego and Sidney. The red and gray sandstones forming the ‘ Oneonta ledge ” near the top of Powell hill, northwest of Oneonta, are important in _ the history of the nomenclature of the New York formations, since they are probably the typical outcrop to which-Vanuxem in 1840 applied the name “sandstone of Oneonta” describing the forma. tion as consisting “of many veins of gray sandstone, and some- times of red sandstone; when weathered it exhibits a peculiar structure, to all appearance owing to the manner in which it was deposited from water; in this rock we often find the remains of terrestrial plants, and sometimes they are thrown together in such numbers as to form a thin mass of coal, extending for a few feet, but only an inch or more in thickness; this rock is found in Otsego, Chenango and Broome counties.” While in his final report in describing the localities where the crossbedded structure of the Catskill group® is shown in the most marked manner he cites “the hillside, near the top, below Oneonta.”¢ ‘As already stated ‘and shown on the section, the writer refers the fossiliferous rocks. in the lower part of Powell hill, at least to the top of D8, 209 feet above the railroad, to the Ithaca formation. Many different cpinions have been expressed in reference to the correlation of these fossiliferous deposits and it may be of interest to recall some ef the more important ones. a 4th an. rep’t third district (assembly document no. 50, 1840) p. 381. b As already explained in his final report Vanuxem referred the Oneonta sandstone to the Catskill formation; a classification that is now abandoned. eGeology of New York. 1842. pt 3, p. 187. 80 NEW YORK STATE MUSEUM In 1841 Conrad named them the Oneonta group,’ while in the | = following year Vanuxem referred them correctly to the Ithaca group.2 In 1885 Prof. Hall published the following classification for the. Devonian system of Otsego, Delaware and Chenango — counties:. e. ‘Catskill group Chemung group Portage group ; Hamilton (upper) : Hamilton group ‘ Oneonta , Corniferous limestone Oriskany sandstone.”¢ The author states that the Oneonta sandstone “comes in at about the close of the Hamilton period, or more properly may be regarded as the result of changes which terminated the conditions of the Hamilton group.”? In the list of localities following the description of species, Goniophora carimata (Con.) Hall from -Oneonta,é Nuculites cuneiformis Con., at Oneonta,’ and Phthoma nodicostata Hall hear Oneonta9 are referred to the Hamilton group. , : In 1886 Prof. H. S. Williams showed. that the fossiliferous rocks at Oneonta belong stratigraphically. above the horizon of the Genesee shale and he called them the Paracyclas lirata stage. Prosser in 1887 showed that between the fossiliferous rocks of Oneonta and the top of the Hamilton formation are the Sherburne flagstones of Vanuxem.' | : a 5th an. rep’t paleontology of N. Y. (assembly doc. no. 150, 1841) p. 31. b Geology of New York. 1842. pt 3, p. 192. c Geol. surv., N. Y. Paleontology, 5, pt 1, Lamellibranchiata 2:518. d Ibid, p. 517. e Ibid, p. 302. F Ibid, p. 326. g Ibid, p. 474. h Proc. American ass’n adv. science, 34: 225, 233 and see §10 of the chart of Meridional sections of ’ the Upper Devonian deposits of New York, Pennsylvania and Ohio. i Proc. American ass’n adv. science, 34: 210. ; . CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 81! _ Darton in 1893 referred them to the Hamilton stating “The basal beds [of the Oneonta] are gray flags which merge into the Hamilton.’ : tae - And again that ‘The Chemung rocks to which Mather and others refer, lie below the Oneonta beds or about 1000 feet below the actual base of the Chemung horizon, and are Hamilton in position. Their fauna is meager and consists of species supposed by Vanuxem to be ‘Chemung’ [Ithaca] in central New York, but now known to be Hamilton.’ ‘The same year, 1893, Prosser published a paper describing sev- eral characteristic sections of the upper Hamilton, Sherburne, and - Ithaca formations in eastern New York accompanied by lists of _ fossils. One of these localities was the Anthony White quarry west of Oneonta from which a list of 20 species with their geologic range was given.© The paper concluded as follows:. “It seems clear to the writer that the above lists of fossils with the state- ment of their stratigraphic position show that the fossiliferous © zone underlying the Oneonta sandstone in Chenango and Otsego counties is not the top of the Hamilton but belongs in the Portage stage.”? By the use of the word stage in the preceding sentence the writer intended to convey the idea that in his opinion this fossil- iferous zone was synchronous with some part of the formation which on the Genesee river is called the Portage; or along the meridian of Cayuga lake is called the Lower Portage, Ithaca and Upper Portage but did not say with which part of that formation it was to be correlated. : 3 On the Geologic map of New York, 1894, the rocks along the Susquehanna river valley above, and for some distance below Oneonta are referred to the upper part of the Hamilton for- mation. XXIII F*. East of the Powell hill section, flowing from the © north through the central part of Oneonta is a stream known as a Am. jour. science, 3d ser., March, 1893, 45: 206. b Ibid, p. 207. Also see Sec. B of fig. 2 on p. 205. where the Oneonta sandstone is represented diagrammatically as resting on the Hamilton formation at Oneonta. ce Ibid, Sep., 46: 226-29. d Ibid, p. 230. 82 NEW YORK STATE MUSEUM Silver creek. About 200 feet above the railroad level, along this. stream is an exposure of bluish shale that breaks upon weather- ; : ing into small, irregular pieces. These shales and those someway xs higher along the bank of the old “race way” are quite fossilif- erous. The following species were collected: 1 Spirifer mesastrialis Hall | (cr) 2 8. mucronatus (Con.) Bill. | mete (rr) 3 Chonetces scitula Hall ee (a) a 4 Camarotoechia stevensi (Hall) H. & C. ae (ry 5 Camarotoechia eximia (Hall) H. & C. Ee ae a 6 Paraeyclas lirata (Con.) Hall | — «@) e re 7 Micredon (Oypricardella) bellistriatus een) Hall = AER) < Ai Ithaca form. PAN te aa 8 Nuculites oblongatus Con. | Gao ee 9 Nucula bellistriata (Con.) Hall var. (rr) 10 Palaeoneilo maxima (Con.) Hall , (rr) 11 Leptodesma sp. : : . (r) 12 Pleurotomaria sp. | ee (r) 13 Bellerophon sp. | Se (rr) 14 Tentaculites sp. Sere 15 Crinoid segments (a) 16 Strophalosia Sp. (rr) 17 Tellinopsis subemarginata (Con.) Hall - . (rr) : 18 Goniophora carinata (Con.) Hall i (rr) ; 19 Coleolus sp. : (rr) | 20 Hyolithes sp. : _ (rr) XXIII F°. Farther up the creek is a calcareous stratum two feet i or more in thickness, merging into a sandstone below and a shale — above. The calcareous part is very hard when freshly exposed but on weathering becomes brown and friable. The shale is — very fossiliferous though the specimens are badly broken and the number of species is small. XXIII F*. From the limestone to the upper exposures, sand- stones and shales alternate with lithologic characters similar to those in F*. The combined thickness of the exposed rocks, F?, F° __ CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 83 and F! is 50 feet. The fossiliferous layers extend nearly to the highest exposures which are 200 feet or more above the White quarry. The following species were collected in this upper zone: 1 Chonetes scitula Hall (r) 2 Camarotoechia sp. 3 (rr) vs Spirifer sp. (rr) 4 Palaeoneilo maxima (Con.) Hall (rr)? 5 Nucula bellis'riata (Con.) Hall var. (rr) 6 (2) Tellinopsis subemarginata (Con.) Hall . (rr) 7 Coleolus Sp. (rr) XXIII X*. On the south side of the Susquehanna river, nearly opposite Oneonta, along the Delhi road and a small brook are ex- posures of the upper part of the Ithaca formation capped by the Oneonta sandstone. At an elevation of about 170 feet above the railroad level on the banks of the small stream are bluish shales alternating with thin sandstones. Some of the layers are slightly calcareous and contain some fossils, though the number of species is small as will be seen by the following list: 1 Spirifer mesastrialis Hall (c) 2 8. mucronatus (Con.) Bill. (ek & Gomophora hamiltonensis (Hall) Miller (?) (rr) Poorly preserved. 4 Edmondia cf. subovata Hall | (r) These specimens resemble fig. 21, pl. 64, Paleontology of New York, v.5, pt 1, Lamellibranchiata 2, which came from the Ithaca group at Ithaca and was referred with doubt to this species. | 5 Homalonotus dekayi (Green) Emm. (rr) These rocks belong in the upper part of the Ithaca formation, which extends somewhat higher. For 80 feet above X? the rocks are mostly covered, when a coarse grained, greenish gray sand- stone outcrops by the side of the highway, and in the field to the southwest is a small quarry. This stratum—X‘4—is 250 feet by the barometer above the railroad level and in its lithologic and structural characters closely resembles the Oneonta sandstone, : and is ee as. fone the eee. Set ae ‘fort ee steep hill along the southern ade of the signe ae Oneonta. Ege . fh . ae eis feet by the barometer above the railroad level. : Me dip at this locality of 24° S, 10° W. The section may b epr sented diagrammatically as follows: ° — én SECTION SOUTH OF ONEONTA xs Red shale Oneonta formation 62’ | X® Greenish gray ss. with some shale stone ee se 1) B07 | x8 Mostly covered ee ees , Probably lthaca apehate nog Ne 170/ wie Ee Xx? Bluieh shales with fossils ee a ata: ene Ithaca formation 4 ue | | 170’ | X1 Largely covered 0’ |__| R. BR. _ level Oneonta station $ About one and one third miles west of the Delhi road the s hill is crossed’ by the Franklin turnpike. Red sandstones ee shales were first noticed along this road 245 feet below its sun _ mit, while at 180 feet below the summit is an exposure of 15 fee 2 of red shale which has colored the road a bright red and has been | quarried to some extent and used for red paint. The reds a a a grays alternate from this horizon to the summit of the road. 2 3. - CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 85 ¥- 'e “West Oneonta. XXIII E!. The western part of Oneonta town- ae ship is crossed by the Otego creek and one of its western branches _is Perry brook which flows through the small village of West Oneonta. About one fourth mile above West Oneonta is an old | mill and along the banks of the creek below and above the mill are very fossiliferous, bluish, argillaceous shales. Loose in the brook are large slabs of sandstone containing numerous large and nicely preserved specimens of Spirifer mesastrialis Hall. The rocks along the creek show a decided dip to the southwest. The "base of these shales is about 105 feet higher than the bridge over _ the Otezo creek at West Oneonta, approximately 1380 feet above the base of the Powell hill section at Oneonta, and three miles northwest: of the base of that section. The fauna is: 1 Spirifer mesastrialis Hall — (c) 2 ges. - mucronatus (Con.) Bill. 3 (rr) are 38. mesacostalis Hall (2) (rr) yee = Camarotoechia eximia (Hall) H. & C. (Gc) ea 5-0: stevensi (Hall) H. & C. (ec) G Chonetes scitula Hall | . ee eee TC. setigera Hall | aC) 8 Orbiculoidea neglecta (Hall) H. & C. (?) (27) - 9 Paracyclas lirata (Con.) Hall ~ ee (a) 10 Prothyris lanceolata Hall (rr) 11 Microdon (Cypricardella) tenuistriatus Hall ; (rr) 12 Palaeoneilo maxima (Con.) Hall | (rr) 13 Modiomorpha subalata (Con.) Hall 7 (r) var. chemungensis Hall The large and elongate form found in the east. 14 Modiomorpha cf. mytiloides (Con.) Hall (rr) This is a small specimen resembling in some respects WM. alta (Con.) Hall as fuily as the above species. 15 Grammysia elliptica Hall (rr) 416-G; nodocostata Hall (rr) The impressions show nodose ridges near the umbo similar to figures of this species. 17 Grammysia constricta Hall : (rr) 18 Goniophora sp. ae (rr) reached 230 feet above the base of the shales forming E}. 86 . NEW YORK STATE MUSEUM 19 Leptodesma rogersi Hall as = ees 20 Actinopteria theta Hall (?) Pie 21 Liopteria sp. Beer a 22 Pleurotomaria sulcomarginata Con. . ye 23 Bellerophon rudis Hall (?) : (rr) : & oe 24 Orthoceras sp. 7 (rr) ay It will be seen that the above fauna corresponds to that of the: = =. bluish shales in the vicinity of Oneonta and these rocks belong in se the Ithaca formation, as well as those occurring by the roadside and along the stream till the upper part of the glen, which crosses" « 2 the township line in the northeast corner of Otego township, is ‘. S wo Otego > RB 2 To the west of Oneonta is Otego township, the southern part of which is in the Susquehanna river valley. The central part is crossed by the Otsdawa creek, which enters the Susquehanna river in the vicinity of Otego-village, and in the northern and western parts and onthe south sideof the Susquehanna river are high hills. A large part of the township is covered by the Oneonta formation — | while the Ithaca formation extends along the Susquehanna river valley to the southwest of Otego village, and the high land in the western part of the township belongs in the Chemung formation. Ithaca formation. UXXIC1. In the eastern part of the town- ship are exposures of rocks along Mill creek to the north of the © river road about two and one half miles east of Otego. At thes. foot of the gorge are about eight feet of bluish shales’ which weather to a slightly greenish tint, and contain some concretions and a few fossils, mostly very imperfectly preserved. Baik - LXXIC2. Above the shales is 4 sandstone stratum ‘two feet thick. This is succeeded by another two foot layer of very irregu- lar structure which, in places, is composed almost entirely of con- cretions. Above are more sandstones, some of which are slightly calcareous and about 16 feet above the concretionary one is a strongly calcareous stratum. The sandstones are about 22 feet thick, above which are argillaceous shales containing fossils - CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 87 | - capped by a sandstone which forms the top of the falls in the glen. The thickness of this entire zone is about 30 feet. From the dif- - ferent layers the following species were collected: 1 Spirifer mesastrialis Hall . (c) 28. mesacostalis Hall (?) (c) 3 Camarotoechia eximia (Hall) H. & C. (c) 4 Paracyclas lirata (Con.) Hall > (rr) 5 Prothyris lanceolata Hall | (rr) 6 Modiomorpha concentrica (Con.) Hall (rr) 7 Nuculites oblongatus Con. : (r) & N. cuneiformis Con. — (rr) 9 Microdon (Cypricardella) tenuistriatus Hall (rr) 10 Coleolus sp. (rr) 11 Fish plates and teeth (r)} _ LXXIC®. From the top of the falls to the top of the cliff there are 50 feet of alternating shaly and thin sandstone layers. These ‘rocks contain some fossils, though the number of specimens and “species is smaller than in those of C?. The species listed below were obtained: i Tropidoleptus carinatus (Con.) Hall (r) 2 Spirifer sp. cee 1 UB 3 Camarotoechia sp. (rr) 4 Paracyclas lirata (Con.) Hall (c) 5 Nuculites oblongatus Con. (?) (rr) 6 Actinopteria sp. (rr) 7 Coleolus sp. (rr) 8 Crinoid segments ) ect) The top of these rocks is approximately 155 feet above railroad level to the east of Otego and the three zones belong in the Ithaca formation. LXXI B’. On the northern bank of the Susquehanna river about one mile east of Otego is a cliff of shales and sandstones some 20 feet in hight. The base reaches water level and for 10 feet is com- posed of bluish shales with thin, slightly calcareous, concretionary layers. Then quite a heavy sandstone stratum occurs with quite arenaceous shales and above this a sandstone stratum a foot or ~ These rocks are ate ron teorguea the Tthaca fe Shindian The species listed below were ec Re: Spirifer mesastrialis Hall Rigetr ess st: 39 Camarotoechia eximia (Hall) HSC 3 Tropidoleptus carinatus (Con.) Hall See ee speciosa (Hall) Beecher aes: 5 Paracyclas lirata (Con.) Hall 2 os E : _ 6 Palaeoneilo sp. Seas : og | a mile x n6 “of one vulage is an puheteee) E=posune because the pass: c | is piety: shown. The level of the creek at the e hid a sing be. fs - east of Otego on the river road is only about five feet lowe: "the railroad level but from this pe to the next a : : “tion is reached there is a rise of 51 feet. By the side of the 3 v at this bridge ahoue three feet of shales are ses which 0 and the fauna is meager. The list is as follows: 1 ~Nuculites oblongatus Con. - .(?) Modiomorpha sp. en 3 (2) Leptodesma sp. 4 Crinoid segments—large size +S. Plant stems —_ _ CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 89 ~ ~ - up the creek a two foot sandstone stratum shows. In the cliff above the covered portion are thin shaly layers of gray sandstone which soon become greenish gray and massive, and about 11 feet above their base is a mass of blue shale in the midst of the massive gray sandstone which is like a channel filling. The gray coarse grained sandstone continues for 37 feet when a stratum of red shale two feet thick is reached, on top of which is -. one foot of red sandstone and above this a one foot stratum of gray sandstone capped by drift. It is evident that the coarse gray sandstone with the red shale and sandstone above forms the basal part of the Oneonta formation. ‘At the upper end of the short gorge, immediately above the third highway bridge is a small quarry in the greenish gray Oneonta sandstone not far 3 below the red shale. At this place a block was found, evidently from the quarry, on which are three well preserved specimens or Amnigenia catskillensis (Van.) Hall. It will be remembered that the above rare fossil is the characteristic shell of the © Oneonta formation to which it is supposed to be confined. This report mentions several new localities at which the shell was found and caréful search would probably serve to increase the number. | | On the hillside 125 feet above the top of the cliff in the above section is a broken sandstone ledge which varies from a few to 20 or more feet in thickness. At the base there is a gray sand- stone followed by a red with gray sandstone again at the top of the ledge. - = . The section along Otsdawa creek may be tabulated as follows: OTSDAWA CREEK SECTION A’ Gray and red sandstone . Concealed BONE rl. — Gray sandstone . S < A PR 2 AS” Red shale and sandstone de a = A+ Greenish gray sandstone Oneonta A® Concealed : : - « | 2 | Shales and sandstones Ithaca ) a | 8’ | Covered | | A? a J Pattee 3’ | Shales at second bridge Sone | ee. as 3 Hit A? OM oaths Covered | .....-| 8° Approximate R. R. level 0’ |———!/ Creek level at river road bridge > ¥ ama Aig » CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 91 A comparison of the elevation of the base of the Oneonta sand- stone in the Emmons section with that of the Ostdawa affords. the means for determining the amount of dip a mile between the two localities. The base of the Oneonta sandstone in the Emmons section is 390 feet above railroad level and in the Ots- dawa section approximately 60 feet. The railroad level at Otego. is approximately 73 feet lower than at Emmons which makes the - Oneonta sandstone approximately 403 feet lower in the Ostdawa glen than in the Emmons section. The two stations are about 9.6 miles apart which wouid give a dip of 42 feet a mile to the ~ southwest. To the southwest of Otego the Oneonta sandstone soon runs. down to the level of the highway and there are frequent ex- posures of red shale and sandstone, alternating with coarse gray- | _ ish sandstone by the side of the highway between Otego and - Wells Bridge in the southeastern corner of Unadilla township. On the Geologic Map of New York the base of the Oneonta sand- stone is represented at East Unadilla which, is probably some three or four miles too far to the southwest. The dip would indicate that the base of the Oneonta sandstone reaches river -level within a distance of less than two miles southwest of Otego. Unadilla This is the southwestern township of Otsego county, situated to the west of Otego and bounded respectively on the south and . west by the Susquehanna and Unadilla rivers which come to- gether at the southwestern corner of the township. The greater | part of the township is covered by the Oneonta formation, the red and gray sandstones being well exposed along a number of the streams. In the Delaware and Hudson railroad cut above Unadilla village is an excellent exposure of the Oneonta greenish sandstone and red shales. The high ground in the northeastern _ part of,the township is covered by,the Chemung while the hill at the southwestern point forming the divide between the Una- dilla and Susquehanna rivers is capped by the base of the Chemung. ; = ware, a nid Chenango counties the first fauna of t ‘ ee which forms the angle between the two rivers na there is only a small exposure of the rock. Ae ea _base of the Chemung. : shales of A® and on its surface are loose, angular slabs, evidently LXXIV A’, To the mOetNanOet of Sidney i is the h i rs _ confluence. uae: are a few exposures on the hillside 9 the Oneonta formation : while the upper part neloneee in mth of tite Chemung. | and sandstone. This Ge of the hill is well need by avift LXXIV A‘. Above this outcrop at an elevation of 110 feet ? small quarry of ee stone eacate as Secor’s Bs in wh Chemung stage consists largely of crinoid segments SO that i seems reasonably safe to refer the rocks of this quarry to t LXXIV A®. Along the field road some 95 feet higher - ane the “quarry are ee yee of bluish Biale in which a few fossils were Tent culties sp.: and crinoid séoncare fauna clearly indicates are in the lower part of the Cnentping formation. The summit of the hill is some 90 feet above the from that vicinity, a few of which are calcareous—like a fire stone—and composed largely of small crinoid segments: and pale of Air rypa reticularis el Dal. In some of the slabs = i a ris (Lin.) Dal., iaumiehe and Teniouiitizes sp. are found face most of them contain crinoid segments. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 93: The section may be represented in the following diagrammatic: manner: ! SECTION OF HILL NORTHWEST OF SIDNEY . 405’ | 90’ | A? Covered to summit of hill slo |———| A® Bluish shale 95’ | A® Covered 220’ |——— 15’ | A* Secor’s quarry. Sandstone and shale = 110’ | A® Covered 95° |\———-| A” Red shale and sandstone 95’ ve ee 0’ River bridge and railroad level The comparison of the section north of Sidney with that of the Otsdawa north of Otego furnishes a means of estimating the - thickness of the Oneonta formation. The distance between the two sections is 124 miles; the Sidney station is 64 feet lower than the Otego while the base of the Oneonta formation on the Otsdawa creek is 60 feet above the railroad level. If we assume that the dip remains the same between Otego and Sidney as between 94 NEW YORK STATE MUSEUM eee eS Emmons and Otego then there is a thickness of 485 feet of rocks from the bottom of the Oneonta formation to the red shales of A? in the section north of Sidney and a thickness of 595 feet from the . bottom of the Oneonta to Secor’s quarry. It is probable that the tep of the Oneonta formation lies between the red shales and the base of the quarry indicating that the thickness of the formation ~ = is between 500 and 600 feet. Bainbridge The next township to the southwest in the Susquehanna river valley is Bainbridge in the southeastern part of Chenango county. ‘The eastern half of the township is crossed diagonally by the river from the northeast to the southwest and the larger part of it is covered by rocks of the Chemung formation, the Oneonta forma- — tion occurring only along the valley of the Susquehanna river and its tributaries in the eastern part of the township. XXXIV At. In the northwestern part of Bainbridge village along the stream from the northwest is a small glen which is quite narrow and for some distance bounded by walls exposing 70 feet of rock, the base of which is about 80 feet above the level of the Park hotel in the central part of the village: The rocks consist mostly of bluish shales and thin sandstones with one or two irreg- ular slightly concretionary strata. “The shales are fairly fossilifer- ous, specially in certain layers, while in the sandstones a smaller number of fossils is found. There are frequently somewhat calcare- ous layers in which occur great numbers of crinoid segments. The lower shales contain numerous specimens of Spirifer mucronatus (Con.) Bill. var. posterus Hall & Clarke which occurs in all of the | vocks of this zone. In the upper part of the glen are layers con- taining many specimens of Liorhynchus globulifornis (Van.) Hall; a smaller number of Productella lachrymosa (Con.) Hall and very large specimens of Atrypa reticularis (Linn.) Dal. The complete fauna of the zone follows: 1 Atrypa reticularis (Linn.) Dal. (a) Broad specimens with coarse plications. Oe SLO// ON Al LAINERIYGL OLIVE SHALES CHEMUNG PARTLY COVER ED. IPREGCGULAAR OLIVE SANDSTONE WITH CONCRFETIONBAYV LAVER. PARTLY COVE ED SHALES ANO SANDSTONE WITH SOME LAVERS COMPOSED OF FOSSILS. COVERED. BLuisH SHALES ANO SANOSTONES WITH ABYNOANT FOSSILS CHEMUNG LOweST AOS, B@Oo7, FG. SLCTLON OF BUMS CAEL A Hh AIOE a z / GULA SSS (| OLWE SHALES AND (RAE # CONGR ETIONBAAY SANOSTONE ae MaosTeLy COVESEO | BAIOGCE OLIvE SHALES AND SAN OSTINES W/TH LAOS a HES p CHEMUNG COVERED LEVEL of SUSQUEHANNA BIVER. —, _ CLASSIFIGATION, ETC. OF HAMILTON AND CHEMUNG SERIES 95 2 Spirifer mucronatus (Con.) Bill. (aa) var. posterus Hall & Clarke Small and very mucronate. Apparently this species. Some of these specimens were examined by Dr Clarke who wrote of them as follows: “ These specimens are more ‘ progressed towards Sp. mesacostalis [than the Ithaca fauna Sp. mucronatus var.posterus]; the internal septum is more pronounced and the median costa stronger. They impress one as distinctly more progressed toward the obey mesacostalis extreme. I have called them posterus; perhaps it would be nearer the truth if one should designate them as posterust+or mesacostalis—. I wouid not call them mesacostalis for the concept which that term embodies is ' a mucronatus with a well developed median costa and in- ternal septum.” 3 Cyrtiina hamiltonensis Hall (rr) 4 Schizophoria impressa (Hall) H. & C. WN. striatula (Schl.) Schuchert (r) 5 Productella lachrymosa (Con.) Hall ste) 6 Liorhynchus globuliformis (Van.) Hall (aa) The specimens are flattened in the shale but I think they are the above species rather than L. mesacostalis Hall. 7 Cryptonella eudora Hall (?) (rr) 8 Leptodesma sp. (rr) 9 Palaeoneilo brevis Hall (?) “(rr) 10 Tentaculites spiculus Hall (?) (a) 11 Crinoid segments and stems (c) These rocks are, clearly, stratigraphically above the Oneonta formation and correspond with those of Greene township along the Chenango valley and as the writer stated in the early part of this report they may be regarded as representing the lower part of the Chemung formation. However before this question can be settled authoritatively the rocks should be carefully studied and followed across the country from the Chenango valley to the southern part of Tompkins county. This fauna was called the Ttorhynchus globuliformis stage by Prof. H. S. Williams who studied specimens from this glen and considered them to repre- ai5th an. rep’t N. Y. state geologist, p. 165. _ sent a modified Hanilida fauna oceurring below the bas eee _ Chemung.¢ a Se 9.0.0 58 Ae Porther up the brook, about one smile Wenaes ae oe _ Bainbridge, a small branch enters it from the south along whi = E ee are exposures of rocks. Ledges also occur along the highw: a short distance farther northwest. These rocks are 150- a 7 abe than the top of the glen; but in general their litholos characters are similar to those in the glen, though there re _ thicker layers which are strongly calcareous and composed lar —_ = ot fossils, specially the. small Spirifer. The following sp were collected: — eS 1 Spirifer mucronatus (Con.) Bill. (?) ; ---var. posterus H. & C. eae Se _ mesastrialis Hall Eee Ss Productella lachrymosa (Con.) Hall 4 Modiomorpha quadrula Hall 5 Schizodus chemungensis (Con.) Hall a aa . var. quadrangulus Hall Sai -___-6_ Lyriopecten tricostatus (Van.) Hall | - (a 7 Bellerophon maera Hall (?) “ | e seve of a rather eiedlng olive sandstone, with a conden to conere 2 ind tionary structure. There are some fossils specially in — ‘certain z layers, the following species having been collected in a few mé ments: . | 1 Spirifer mesastrialis Hall 2 Productella lachrymosa (Con.) Hall | 3 Schizodus chemungensis (Con.) Hall mee var. gquadrangulus Hall 4 Spirifer mucronatus (Con.) Bill. var. posterus H. & C. : p aProc. Av. ass’n for the adv. science, 1886, 34:226, 231 and Sochien 10 of the chart ayia on the Meridional sections of the upper Devonian deposits of New York, Pennsylvania — and Ohio. * CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 97 At the top of the hill over two miles forthwest of Bainbridge and 135 feet above the base of the concretionary sandstone, olive shales outcrop by the side of the highway. On the accompanying section these shales are called A®. No fossils were discovered though this may be due to the fact that very little time could be spent in searching for them. LXVIII C1. Near the southeastern corner of Bainbridge is the small village of Bennettsville just below which on Bennett’s creek is a mill. On the north bank of the creek directly above the highway and below the dam are ledges of thin sandstones and biuish, slightly arenaceous shales containing small Lamellibranch shells of which Leptodesma sociale Hall, Orthonota undulata Con.,, and Uunulicardium fragile Hall are the most common. Fossils are not abundant and though in the upper part of the exposure some calcareous layers, composed largely of crinoid segments, are seen, still none of those strongly calcareous layers containing numer- ous Brachiopods, that occur rather frequently in the fossiliferous | beds of the lower Chemung of this region, were found. The base of the rocks is approximately 65 feet above the level of the Susquehanna river, and in the bank 29 feet are exposed. The following species were collected: 1 Produciella lachrymosa (Con:) Hall (?) : (rr) Broken specimen very similar to this species. 2 Orthonota undulata Con. ee) 3 Leda diversa Hall | (r) 4 Modiomorpha quadrula Hall (r) 5 Lunulicardium fragile Hall (c) 6 Grammysia zonata Hall (?) , (rr) 7 Leptedesma sociale Hall , (c) 8 Leptodesma sp. (rr) 9 Nucula sp. (rr) Very small specimen, unlike any of the figures. 10 (?) Prothyris sp. (rr) 11 Crinoid segments | } ey (c) ~ - eastern township of Chenango county, which is bounded on the — Bennettsville loose on the surface and in the stone walls are. numerous blocks composed to a large extent of fossils. Spe rae cially abundant are Spirifer mesastrialis Hall and 8. mucronatus — Sr" = (Con.) Bill. var. posterus H. & C. There are also some specimens eee of the large Lamellibranchs of the Chemung, as Lyriopedene tricostatus (Van.) Hall.. A farmer residing in that neighborhood — ee stated that the fossiliferous blocks or the “shell rocks” as we ? ne = called them were more abundant on the northern than on the — Ras, southern side of the creek. From loose blocks in this vicinity — a the following species were collected: pe i 1 Spirifer mesastrialis Hall ee SE mucronatus (Con.) Bill. te. | (aa) ore var. posterus H. & ©. | 4 ed oe 3 Liorhynchus globuliformis (Van.) Hall ee oe : 4 Schizophoria impressa (Hall) H. & C. ~ ee an 5 Modiomorpha quadrula Hall . | 7 ep oes fe 6 Sphenotus cf. contractus Hall ae Go (eS cf. clavulus Hall iF ee Pig (rr) mes Both species imperfectly preserved. 8 Lyriopecien tricostatus (Van.) Hall ei RIS fe). oe = i 9 Oyrtina hamiltonensis Hall | ae oe mo 10 Bellerophon maera Hall — ae 1s iM Afton ee z i To the south of Bainbridge and Coventry is Afton, the south- + east by Delaware county and on the south and partly on the ow west by Broome county. The township is crossed diagonally me from the northeast to the southwest by the Susquehanna river, Ne the largest tributaries of which are from the north. Two of ) these, Bump’s creek and Kelsey brook, unite near Afton village; ie while the third, Wylie brook, crosses the extreme western part | of the township. Beg LXIX At. About one mile above Afton on the south ae: the | Susquehanna river and from 20 to 25 feet above its level a few ‘NOLAY ‘“MOOUd AWSTIHY NI DNOWHHO AO MAIA - CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SHRIHS 99 feet of fossiliferous olive shales and thin sandstones are exposed ‘by the side of the highway. Only a brief search was made and the following list might undoubtedly be increased: 1 Spirifer mucronatus (Con.) Bill. (r) var. posterus H. & C. 2 Produciella lachrymosa (Con.) Hall (c) 3 Stropheodonta demissa (Con.) Hall La (rr) 4 Grammysia undata Hall (?) | : 3 (rr) Broken specimen. 5 Liorhynchus globuliformis (Van.) Hall | 2 rr). 6 Lamellibranch ? (rr) Too badly broken to be identified. These rocks are clearly above the Oneonta formation and in the zone which is referred in this report to the lower part of the Chemung. Darton in describing the Oneonta-Chemung bound- ary from Franklin, Delaware county westward, said: “It ex- tends along the slopes south of Unadilla and Sidney down the Susquehanna toa couple of miles below Afton.”* On the Geologic map of New York the top of the Oneonta formation is represented as extending down the Susquehanna river valley rather more than two miles below Bainbridge to the mouth of Bennett’s creek and up this creek to the vicinity of Bennettsville. If this line be correct then the rocks of LX VIII C! in the creek below Ben- nettsville must be quite near the bottom of the Chemung. LXIX B*. To the north of the village of Afton is a rocky gorge in Bump’s creek, the lower end of which is scarcely one fourth mile from the center of the village. The base of the rocks at the lower end of the gorge is 50 feet above the Susquehanna river, and some 85 feet are shown along the gorge, the upper. 10 feet being by the roadside above Pixley’s mill. The rocks consist mainly of olive shales alternating with sandstones six inches to one foot in thickness. There are some quite calcareous layers composed largely of shells; one of these occurs in the gorge just below the Pixley mill in which are large numbers of specimens . aAm, jour. science, 3d ser., 45:207. 100 NEW YORK STATE MUSEUM of Spirifer mucronatus (Con.) Bill. var. posterus Hall & Clarke, - and numerous specimens of Productella tachrymosa (Con.) Hall. | A little above in a thin sandstone are a considerable number of specimens of a large Schizodus, referred to S. chenvungensis (Con.) Hall var. gquadrangularis Hall. In the bed of the creek is a some- what concretionary contorted stratum below the calcareous one | which is thicker than the majority of such strata in the Hamil- : ton and Chemung series of eastern New York. This is a good ae locality for collecting in the lower Chemung as the following list _ . oy will show: 1 Spirifer mucronatus (Con.) Bill. Le ae ae var. posterus H. & C. se 3 28. — mesastrilis Hall = S0ee} 3 Productella lachrymosa (Con.) Hall (a) 4 Schizophoria impressa (Hall) H. & C. (rr) 5 Liorhynchus globuliformis (Van.) Hall . (r) 6 Camarotoechia contracta (Hall) H. & C. (aa) 7 Schizodus chemungensis (Con.) Hall | (c) var. quadrangularis Halk These are rather large specimens 43 mm long and 35 mm high but this is the only species similar in outline. 8 Palaeoneilo brevis Hall . (a) # var. guadrangularis Hall Abundant on one slab. ts ag filosa (Con.) Hall var. - (rr) The concentric striae are fine all over this species until the posterior slope is reached when they suddenly become sharp and angular. 10 Sphenotus sp. (rt) Small and poorly preserved. 11 Grammysia cf. undata Hall (r) Broken specimens. 12 Ectenodesma birostratum Hall (rr) 13 Lyriopecten cf. priamus Hall | (r) The ribs of the large specimen have finer striae on them and a smaller rib alternating with the larger ones. 14 Bellerophon maera Hall (?) (rr) 3 —i > 5 3 ove Mes ~ ae 7 =f i - yas 2 CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 101 15 Bryozoan sp. — Parr) 16 Goniophora chemungensis (Van.) Hall (?) (rr) Only one specimen and that smaller than the normal forms. 17 Stropheodonta demissa (Con.) Hall (?) (rr) 18 Lyriopecten tricostatus (Van.) Hall : (rr) 19 Schizodus chemungensis (Con.) Hall (rr) 20 (?) Microdon (Cypricardella) sp. (tr) A large but broken specimen. LXIX Bt. For some distance up Bum p’s creek, above the gorge, there are no exposures; but about one and three fifths miles northwest of Afton there is a fair outcrop of sandstones and 7 bluish to olive shales. The base of B‘ is some 95 feet higher than - the top of B? or 230 feet above the Susquehanna river, and 10 feet of rocks are exposed. The top of the exposure is at the highway bridge on the cross road just below the dam. One irregular, con- torted sandstone layer was noticed, as well as a calcareous one composed largely of shells. There is a tendency in the shale to : split across the bedding as well as along its plane so that it breaks into thin, narrow strips. Fossils are common specially in the bluish, somewhat arenaceous shales to thin sandstones, Spirifer mucronatus (Con.) Bill. var. posterus H. & C., Liorhynchus globuliformis (Van.) Hall and Productella lachrymosa (Con.) Hall ‘being the most abundant. The entire list follows: 1 Liorhynchus globulifornis (Van.) Hall — (c) 2 Productella lachrymosa (Con.) Hall : (c) 3 Spirifer mucronatus (Con.) Bill. var. posterus H. & C. (a) 4 Camarotoechia congregata (Con.) H. & C. (?) (a) These specimens are rather intermediate between the above Species and. C. contracta Hall. 3 Stropheodonta demissa (Con.) Hall (rr) 6 Microdon (Cypricardella) cf. bellistriatus (Con.) (rr) In form and size like the above but the striae are like those of M. tenuistriatus Hall. 7 Palaeoneilo brevis Hall (rr) 8 Palaeoneilo sp. (rr) ; 10 Lyriopecten tricostatus (Van.) Hall eget ee -- 11 Bellerophon maera Hall : (ry Et 12 Pleurotomaria sp. ee a (ery eae Very imperfectly preserved. in 13 Orthoceras leander Hall (?) : (ry oS : 14 Modiomorpha quadrula Hall Ses 102 NEW YORK STATP MUSEUM _ 9 Leptodesma sociale Hall The rocks described above, from along Bump’s creek, are in the = lower part of the Chemung as it has been defined in this report — and this creek together with the one at Bainbridge affords ce fair opportunity for the examination of this part of that forma-_ tion. The creek valley was followed from above Bt at the saw. <= = ets mill to a point near the township line between Afton and — ae Coventry; but it is fairly broad and somewhat marshy and the rocks are covered with drift so that no further exposures of noe importance were seen. ee LXX At. To the north of Harpersyille is a brook whose souther- “ ly course is near the township line between Afton and Colesville. : ; On the bank, a short distance above the iron railroad bridge on —__ the Binghamton division of the Delaware and Hudson railroad, — are olive shales, most of which are somewhat arenaceous, and. sandstones which are mainly in a contorted layer. . The base of the exposure is about 70 feet below the Harpers: ville station and only a few feet lower than that at Afton. Spirifer mucronatus (Con.) Bill. var. posterus H. & C. is common in these shales while in loose blocks along the creek are numerous specimens of Spirifer mesastrialis Hall. The following additional — species were found in the loose pieces: 1 Spirifer mucronatus (Con.) Bill. (ay var. posterus H. & C. 2 Productella lachrymosa (Con.) Hall | (r). 3 Camarotoechia cf. congregata (Con.) H. & C. ? (Chee 4 Grammysia communis Hall (rr) LXX A*. Farther up the stream and 40 feet above the base of A! is an exposure of greenish to olive sandstone on the bank of CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES. 103° the brook with some bluish arenaceous shales at the base. In the sandstone is an irregular concretionary layer and the thick- “ness of the rocke exposed at this locality is 10 feet. . No fossils were found. LXX A5, Along the main brook no further outcrops were found above A® for the valley seems to be quite deeply covered with drift; but in a small run from the-west and nearly west of ared schoolhouse are outcrops of shales and sandstones. The base of this zone is 115 feet above the top of A? and for 95 feet there is a nearly continuous rock section consisting mainly of thin bedded sandstones in layers six inches or more in thickness with some - layers of irregular structure and arenaceous shales. In the upper part are greenish to bluish shales that are more argil- laceous in character and there are occasionally thin, rather strongly calcareous, abundantly fossiliferous layers in one of which Bellerophon maera Hall is common. The following species © were obtained at this locality: 1 Liorhynchus globuliformis (Van.) Hall (r) 2 Bellerophon maera Hall ~ : (c) Common in some very calcareous layers. 3 Grammysia sp. Bote: (r) 4 Palaeoneilo brevis Hall (r) a -P: plana Hall (rr) 6 Modiomorpha quadrula Hall 3 (rr) 7 Leda brevirostris Hall (rr) . 8 Leptodesma sociale Hall (r) For 110 feet from the top of A® nearly to the top of the hill the rocks are covered by drift and soil and no higher outcrops were found at this locality. The section may be represented diagrammatically as follows: _ SEOTION NORTH OF HARPERSVILLE LXX ye: 110’ ~A6 Covered nearly to the top of the hill Rr 3 Mt . A*® Sandstones and shales for most of the d : pay | | along the run : | + x a od ~| 115’ | A* Covered A® Sandstone with shale at base A? Bocned A' Olive shales “ s; ou ———1 Creek level above railroad bridge © FES: ae The divide between the Susquehanna and Chenango river: _. which crosses the western central part of Colesville townshi ete oe _ from north to south is quite heavily covered by drift so that | - outerops of rocks are rather infrequent; but along the streams 7 on the western side are occasional exposures; those in the vicinity : ane of Osborne Hollow, near the western line of Colesville township, ee : were described in part 1 of this report*, and to the west near the Bee top of the high hill south of the Chenango river below Port Cran «ah f a: “ ailith an. rep’t N. Y. state geologist, p. 160-62. Sy Z oy AND PALEONTOLOGIST 17% REPORT OF STATE GEOLOGIST ie CATSKILL WYNKOOP HALLENBECK CHAWTOAD 9 STATE PRINTERS Ti t) OONVNGIHO UNIVERSITY OF THE STATE OF NEW YORK 2 ea = a oI = o - FISHER LEGEND WIL \\\ ONEONTA ITHACA DELAWARE COUNTY WH SCALE awOoOoOu a an AT pe = somes oe aiid ae eae , sprees Ri a declan ~ a rs A x fi aa tl u BS. i. Pte ' , a *. i , Be * \ ct ‘ | R % ae, Mie the std ve i . y day ya r ‘ * en She across Masonville township are in the Chemung formation. Bo Sidney Sidney is the northwestern township of Delaware county, being | situated north of Masonville and south of the Susquehanna river. oe It is bounded on the north by Unadilla and Otego townships, as = Otsego county, and on the east by Franklin township, Delaware : county. The central part of the township is crossed by Carrs creek, which flows from the southeast toward the northwest — and enters the Susquehanna river opposite the village of Una dilla. On*the southern side of the creek are quite steep hills — forming the divide between it and Bennett’s creek. | The creek valley and this range of hills afford occasional sections, though Z rs the rocks are largely covered by soil and drift. = CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 107 LXVIi B2. At the three corners on the northern side of Carrs creek nearly two miles northwest of Maywood (formerly Sidney Center) is an exposure of thin bedded red sandstone. One foot or more of the stratum is shown in a small brook just north of the highway; the top of which is about 33 feet above the level of Carrs creek. This outcrop is in the Oneonta formation and. near its top as is shown by the exposures in the railroad cut on the southern side of the creek. = LX VII Bt. On the southern side of Carrs creek, two miles. northwest of Maywood, is quite an extensive railrvad cut the base of which is 95 feet above the creek level. The rocks shown in the cut are mostly olive shales and sandstones with some _ blue shale. At one place is a spot of shale which is somewhat reddish, perhaps from weathering, but olive at each end. A _ contorted layer of sandstone occurs, and the cut shows a section _ 33 feet in thickness. Fossils are not common, with the exception | of Crinoid segments, but the following species were found by Mr William L. Fisher: ; 1 Spirifer mucronatus (Con.) Bill. (ec) var. posterus H. & C. Poorly preserved. 2 Orthonota (?) parvula Hall (rr) 3 Sphenotus cf. contractus Hall | (rr): 4 Goniophora cf. Hamiltonensis Hall (rr): 5 Tentaculites cf. spiculus Hall gees Cy Abundant on some layers. 6 Large Lamellibranch very poorly preserved | (rr): 7 Crinoid segments (a). Small segments abundant on some layers. The rocks exposed in this cut are near the base of the first fossiliferous zone above the Oneonta sandstone which, as already stated, is referred to the base of the Chemung formation in this: report. At the maximum the base of the cut can hardly be more 108 NEW YORK STATE MUSEUM. ee | ee than 60 or 65 feet above the top of the Oneonta sandstone. The e : _ above section may be tabulated as follows: aS are ee ee | | ~ : : 33’ | Bt Olive shales and sandstones. ae nek Chemung baat 95’ 5 62’ | B® Covered ao. 1’ | B? Red sandstone. Oneonta ~ ) | _ 82’ | B® Covered’ A 0’ ae Level of Carrs creek The above section agrees fairly well with exposures near Youngs, one mile farther northwest, where in the railroad cut directly north of the station there are olive and bluish fissile shales alternating with thin, irregular sandstones. There are also irregular, concretionary. sandstones. Fossils are rare, but a few specimens of Atrypa reticularis (Lin.) Dal. were found. In a quarry about 60 feet below the railroad track on both sides of Ford creek are unfossiliferous coarse gray sandstones which split quite regularly making small flags, and an occasional layer of clay pebble conglomerate. In the creek just below the quarry are large slabs of red sandstone which are probably about in place. The rocks of this quarry belong, apparently in the Oneonta formation. About 75 feet lower on the western side of Carrs creek there is a steep bluff in which large masses of angular red sandstones SS NoblAkB. SECTION THROUGH MAY WOOL 70 TOP OF E.. MASONVILLE HILL TOP OF Hite COVE RED GAAVISH THIN-BECCEO SANOSTINE AED sanosrone CATSH/LL COoveEZEO THIN-BEQOED sSAnwosTove CovEREO GRAY SANDSTONE AND OLIVE SHALE CHEM UNG CoveRED GAAVISH TO OLIVE SANOSTONE CovereD OLIVE SHALES AND THIN SANDSTONES Maywooo A&A. cur CHEM UVG MAINLY COVERED = ~ m= SS SSeS oe ree Beo ruin sanestoneE ONEONTA Levet of Cara's CAEEX 2 M1 BELOW Maywoon Na bl Ab hl. SECTION FROM BELOW MAY WOLD MWe MALO 70 TOP OF HILL 8: OF FRANKLIN STATION TOP OF HILL. THIN-BEDOED OLIVE TO LIGHT GRAY SANDSTONE. CHEM UNG. MAINLY COVERED. OLIVE AND BLVE AAGILLACE OVS SHALES NWO SANOSTONES ; Foss1ts./RPANHLIN AF Cur: COVERED. OLIVE SHALES AND SANOSTONES. COVERED OLIVE SHALES ano THIN SAN OS WITH FOSS /L.S Me eoed M Ay wooo 4.4. Cur CHEMUNG MAINLY COVERED REO THIN sAnostoneE ONEGNTA Lever oF Carrs CREEH 21. BELOW MAYWOID, v - CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 109: occur. They are hardly in place, still from their very angular shape and the large number of them they must form a ledge in that immediate vicinity. LXVII A*. In the cut immediately west of Maywood station (formerly Sidney Center) on the New York, Ontario and Western railroad there is an exposure of .84 feet of thin sandstones alter- nating with shales. Some of the thin layers contain large num- bers of Crinoid segments, and the rock being quite calcareous becomes rotten on weathering and turns from a greenish to a brownish color. Some of the shales when weathered are olive but on a fresh surface are mostly bluish. The bottom of the rail- road cut is at about the same level as the Maywood station which is 13888 feet A. T. The dip varies for the different strata exposed in this cut; for one stratum dips about 1° nearly s. e., while that of a lower thin sandstone stratum varies from 14° to 24° S. 10° E. In number of species and specimens Lamellibranchs. _are most abundant though other fossils are common. The list is as follows: 1 Lhorhynchus mesacostalis Hall : | | (rr) 2 Camarotoechia cf. stevensi (Hall) H. & C. (rr) Broken and imperfectly preserved. 3 Spirifer mesastrialis Hall (r) 4 Palaeoneilo constricta (Con.) Hall (rr) ae. Sp. (c) 6 P. plana Hall (?) a (EER 7 Nuculites oblongatus Con. (rr) 8 Orthonota (?) parvula Hall. (r) 9 Leda diversa Hall (c) 10 Sphenotus cf. contractus Hall | (a) 11 Grammysia cf. communis Hall (rr) 12 G. elliptica Hall ' (rr} 13 Leptodesma cf. sociale Hall (Che 14 Ptychopteria sp. (rr) 15: Lunulicardium fragile Hall eh (rr) ~ai att = Aero stones were noted at the horizon A‘* which is estimated as ATS ( ‘road cut at 67B‘, two miles farther northwest, and is, conse- ‘described the top of the Chemung formation, the thickness of 110 NEW YORK STATE MUSEUM ~*~ 16 Orbiculoidea sp. ea ee, Imperfectly preserved. *e ert prs. 17 Orthoceras sp. 18 Crinoid segments . | On some layers immense numbers of small segments. i The base of this cut is approximately 199 feet above the red fs : sandstone of 67B2, or 137 feet higher than the bottom of the Ee quently, at least that much higher stratigraphically in the Che: mung formation. > phe high hill to the west of Came creek, south of Maynor affords an opportunity to measure the thickness of the Chemung _ _ formation. A section has been constructed showing the rocks =e ‘from the level of Carrs creek at 67B! to the top of the high hill | near the Sidney-Masonville township line south of Maywood. The , ! course of this section from Maywood south is up the valley of ee Carrs creek to the first road turning west and then over the eas es to East Masonville. Unfortunately in measuring the section that — route was not followed so that the covered zone called A? and estimated as 209 feet in thickness may vary to quite an extent from that approximation. On this hill the grayish to olive sand- feet above the level of Carrs creek at B1, and they continue to : - at least an altitude of 615 feet the last 80 feet of which are com- posed largely of rather coarse grained grayish sandstone and | some olive shale. This zone is apparently in the Chemung al- though a hasty search was not rewarded with fossils. Suppos-— a5 ing B? to be the top of the Oneonta sandstone and the zone just — : the Chemung in this section would then be approximately 580 feet. From the bottom of the railroad cut at B4, which is un- questionably in the Chemung, to the top of A‘ is, approximately, 510 feet. Above A® for 190 feet the rocks are covered when ~ a 15 feet of thin, irregularly bedded, rather fine grained grayish to greenish sandstone occur in zone A’. The first ledge of red Sandstone and shale seen on this hill which is clearly in the CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 111 Catskill formation is found 52 feet higher. A piece of loose sandstone containing a specimen of Spirifer mesastrialis Hall was found below the ledge of red sandstone but I am hardly inclined to think that it came from the upper part of this hill. 57 feet above the red sandstones and shales occurs another _ ljedge—A—of grayish thin bedded sandstones which are 939 feet above the base of the section. The rocks are then covered for 26 feet, nearly to the summit of the hill, making a section of approximately 965 feet which extends from the upper part of the Oneonta sandstone into the lower part of the Catskill formation. LXVII C1. The section C is in the vicinity of Franklin Station’ on the New York, Ontario and Western railroad, three and one half miles southeast of Maywood and near the line between Sidney and Franklin townships. On the bank of the small brook below Franklin Station and east of the railroad cut is a 10 foot ex- posure of olive to gray colored sandstones and shales containing | plenty of Crinoid segments with a few other fossils. The rocks | are in the Chemung formation. LXVII GC. In the railroad cut aboutone quarter mile northwest of Franklin Station is an exposure of 28 feet of rocks the base of which is 66 feet above C1. The rocks consist of rather thin layers of sandstone alternating with olive and blue argillaceous . shales. In the lower part of the cut is a stratum composed partly of shale and partly of sandstone which has very irregular struc- - ture and is probably somewhat concretionary in form. The dip varies from 24° to 34° S., 20° E. In some of the layers fossils are common and in the rather thin layers of sandstone quite a number of specimens of Spirifer mesastrialis Hall were found. The thin olive shales and sandstones quite closely resemble, litho- logically, the typical Chemung rocks of southern New York. \ The fauna of this zone is as follows: 7 1 Spirifer mesastrialis Hall 3 (c) 2 Atrypa reticularis (Lin.) Dal. (rr) 3 Goniophora subrecta Hall (c) 112 NEW YORK STATE MUSEUM 4 Palaeoneilo brevis Hall | _ 5 Leda cf. diversa Hall Ps 6 (?) Grammysia zonata Hall 7 Lyriopecten priamus Hall : - (rr) : < ; 8 Onychodus hopkinsi Newb. ‘e (Fs 9 Dinichthys tuberculatus (?) Newb. (rr) ie The last two specimens were identified by Dr Eastman. LXVIIC®. There are but few outcrops on the hill to the south of Franklin Station, its slope being well mantled by the drift. — However on the summit of the hill one mile south of the station s is a ledge of thin bedded olive to light gray sandstone which splits into quite thin layers at the surface but thickens as the unweathered part is reached. A small excavation has been made exposing four and a half feet of the ledge. There is an occasional fossil, fragments of Brachiopods and ? Cladochonus -sp., which indicates that the top of this hill is in the Chemung formation. | ! : A section based upon barometric readings has been con- structed from the level of Carrs creek at B! along the creek valley to C! near Franklin Station and then to the top of the hill ‘south of the station. Without making any allowance for the dip which would increase rather than diminish the thickness of the rocks, it will be seen that from the top of the Oneonta red sandstone B? to the top of the hill C® south of Franklin Station | there is a thickness of 547 feet. Or from the base of the railroad cut B‘, two miles northwest of Maywood, which is in the Che ~ mung, to the top of C’ south of Franklin Station there is a thick- ness of 485 feet. The top of the hill C® south of Franklin Station is near the same elevation as the top of zone A® on the hill south: of Maywood which was also referred to the Chemung, and it seems hardly probable that C® extends to the top of the Chemung. This section along the N. Y. O. & W. railroad indicates that for Sidney township the Chemung formation has a thickness of more than 500 feet. : . ee a teks Bia! Salk BE cpa ae Ne Pn ee NLS EON UNE Pe ae ee et i ee <.% gt Oe” eee Aes Lio SSS eh ee ee ee Ee ee eR ee De A a ~ a ea - CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 113 Franklin To the east of Sidney is Franklin township, which is bounded on the north by the townships of Otego and Oneonta, Otsego county. The principal stream is Ouleout brook which crosses the township in a general direction from the east to the west and flowing across the northern part of Sidney township enters the Susquehanna river between Unadilla and East Unadilla. XXXIII B!. In the southwestern corner of the township is the tunnel on the New York, Ontario and Western railroad about half way between the Merrickville and North Walton stations and two excavation of the tunnel the railroad crossed the ridge by means and one half miles southeast of Franklin Station. Before the of a “zig zag” which served as the name of the locality. This — ridge forms the divide between the head waters of the streams entering the Susquehanna river on the north, and tho-e flowing - into the Delaware river on the south. The floor of the tunnel is” 1764 feet A. T. at the southern end and it is 1636 feet in length. ~ The approach to the southern end shows about 40 feet of solid rock consisting of fairly massive and shaly sandstones alternat- ing with arenaceous and argillaceous shales. The lower rocks | are mainly of bluish gray sandstone, then at the middle of the cut are red shales and sandstones from 10 to 15 feet in thickness and on top of these grayish to greenish and bluish sandstones and shales. To the south of the southern end of the tunnel and only a short distance north of the North Walton station large quantities of rock taken from it were dumped. Red shale ap- parently predominates, though there is a large amount of green- ish to bluish shale in which are numerous specimens of Lamelli- branch shells. In a rock slightly more irregular in texture - plenty of fish scales and bones were found with which were as- sociated Lingula and a few other shells. Archaeopteris and frag- ments of other plants were found in argillaceous shales on the dump and in the approach to the tunnel. The northern end of the tunnel is lower than the southern and in the approach it is all massive greenish gray sandstone of somewhat irregular bedding { - came from red, argillaceous shales while the massive greenish : s — Re Sy Ss } rs ; % 114 _ NEW YORK STATE MUSEUM 4 es i ¥ 4 a4 with shale partings. Only a few rods north of the entrance to Se sans the tunnel on the east side, Lingula associated with plant stems tee ee was found in place, while in some of the greenish shales speci- sh gat mens of Liorhynchus occur. A little west of the highway and ~ railroad is a quarry of coarse greenish gray flagstone in which . some of thé layers have a slightly’ pinkish tint. To the north of the tunnel is quite an extensive fill, the material for which came from it, and when first visited about two months after the opening of the tunnel in 1891, there were plenty of large blocks | of red shale to be seen which contained numerous specimens ~ ot Lingula and other shells associated with the bones and scales of fish. When visited in 1895, however, the fossiliferous _- shales taken from the tunnel and dumped at both the northern ~ and southern ends were so badly slacked by weathering that collecting was very unsatisfactory. It is possible that deeper blocks may yet remain unweathered from which fair specimens: might be obtained. The rocks from this tunnel are probably in the lower part of the Catskill formation and affording quite an extensive fauna they become important from a paleontologi- cal standpoint. In fact quite a good many of the specimens _ 3 3 gray sandstone below the red at the northern end of the tunnel resembles the coarse sandstones of the Catskill. The ichthyic re- _ mains were studied by Dr C. R. Eastman of Harvard university, 4 the well known authority in ichthyic paleontology who kindly © prepared the interesting account of these fossils given at the close of this report. He identified Bothriolepis minor Newb. and Onchus sp. Eastman. - : XX XIII A’. The village of Franklin is located in the valley of Ouleout brook from 400 to 500 feet lower than the New York, Ontario and Western railroad tunnel between Merrickville and ~ North Walton. A mile and a half below Franklin a brook enters the Ouleout from the south and a section was constructed from the Ouleout level to the top of the hill on the south between the Franklin Station and Merrickville highway. The rocks along the valley of Ouleout brook are very largely red N0.35,A.SLCTIOW SOUTH OF LRANALIN TOP OF WILE GRE ISH-GBAY SANOSTONE a CATSHILL NEAR LEVEL OF QEW. TUNNEL 590| Cove rea. loose focH wirH CHEMUNG rossite. FEO SHALY SANOSTONE. GREENISH SANOSTONE, FED SAN OSTOME., N0.68,2.8EC07/0N NOARTHWE LT OF TELM MSN LAE Vahe MOSTLY COVERED 79¢| GAEENISH AND FEO AAGILL ACEOUS SHALES = WITH FOSSILS. 3 20 | THINGREEWISH sANosTonE GHEMUNG LEVEL OF SPRING LAHE q OF /55| COVERED AED SHALE ONE ONTA 1454S; MOSTLY COVERED. AH. | Decry Posr OFFICE ~ a Me ‘i . 9 . ~ CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 115 argillaceous shales with some sandstones belonging in the Oneonta formation. Along the brook and highway from the Ouleout valley toward Franklin Station the rocks are partly covered for 130 feet, reds showing now and then, when a con- spicuous red sandstone crosses the brook. 60 feet higher and _ just below the forks in the road is an outcrop of red, shaly sand- stone alternating below with greenish layers of sandstone. -This locality is about two miles from the tunnel and is, apparently, at about the top of the Oneonta formation. Loose along the brook and in the fields are numerous blocks of sandstone con- taining large numbers of Crinoid segments. Unfortunately the northern slope of the hill is generally deeply covered with drift and no exposures of these fossiliferous rocks were found. From loose blocks in the side of the hill the following species were collected: 1 Goniophora chemungensis (Van.) Hall | (rr) 2 Palaeoneilo constricia (Con.) Hall (r) 3 Nuculites cuneiformis Con. (rr) 4 Leptodesma sociale Hall : (rr) 5 LD. Sp. ; (rr) 6 Camarotoechia sp. (rr) 7 Pleurotomaria sp. (rr) 8 Tentaculites sp. : (rr) > 9 Crinoid segments (aa) Very abundant in some of the pieces. They belong, however, in the Chemung formation which was estimated by Darton to “ have a thickness of about 300 feet ’% to the south of Franklin. At 590 feet above the top of the Oneonta red sandstone noted in the brook is a ledge of greenish gray sandstone somewhat unevenly bedded (A‘) near the top of the hill which is some 55 feet higher, and on its surface are numerous blocks of red sandstone. No red rock was found in place, but. as this hill barometrically is some 190 feet above the Merrick- ville station it seems probable that its upper part, including the a Am, jour. science, 45: 207. 116 a NEW YORK STATE MUSEUM > coarse, greenish gray sandstone of A‘, is in the Catskill forma-_ a tion. However, farther to the east and on the other side of the __ small valley are thin bedded, grayish sandstones near the summit : _ of the hill, which contain occasional small Crinoid segments. To = the east of the road north of Merrickville at the above locality there is a ledge of this sandstone eight feet in thickness, and re < about 25 feet higher on the highest point of the hill are ledges of coarser grained grayish sandstone. On the western side of zs the road at the head of the small brook and narrow valley and 80 | woes feet lower is a ledge of finer gray sandstone some 15 feet in thickness. | | ‘ag XXX D?. One fourth mile south of Franklin village is a steep . and rather high hill between the Ouleout and Handsome brook _ valleys known as Round Top. The lower part of the hill being somewhat covered only occasional outcrops of red and gray sand- 2 stones and shales occur and at an altitude of 234 feet above the | level of Ouleout brook is a stratum of breccia, eight inches or _ so in thickness, above which is red sandstone. The red rocks continue to 332 feet where the last ledge of thin, red sandstone was seen. 10 feet higher is the bottom of D*, a zone. composed of slightly greenish to grayish thin bedded and shaly sandstones — which continues for about 45 feet to the top of the hill. Some ~ -of the layers contain fossils the most abundant being crinoid — segments but Atrypa reticularis (Lin.) Dal., several species of Lamellibranchs, and, fragments of fish were also found. The top of this hill is clearly in the zone which is referred to the lower part of the Chemung in this report. The following species were found in the shaly sandstones of D?: | 1 Atrypa reticularis (Lin.) Dal. (r) 2 Sphenotus contractus Hall (?) | ' (rr) 3 Grammysia eliptica Hall (er) 4 Edmondia cf. philipi Hall | (c) aad ip cf. subovata Hall (rr) 6 Goniophora subrecta Hall | (rr) % Prothyris cf. lanceolata Hall ae (rr) CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 117 8 Lyriopecten sp. ) | | : (rr) Poorly preserved specimen. 9 Orthoceras sp. — | (rr) 10 Crinoid segments (c) 11 Fish scale (rr) SECTION OF ROUND TOP HILL XXX D 387’ |——-—| Top of Round Top 45’ | D® Greenish to grayish sandstones. Chemung ———| First fossils oy. 1a Last red sandstone 98’ | D® Red and gray sandstone 934’ |——_—} Breccia layer Oneonta 234’ | PD} Partly covered Red and gray sandstones and red shales i= =F Level-ot Ouleout creek Franklin township has occupied a rather conspicuous position in the geological literature of Delaware county since the an- ‘nouncement of the discovery of fossils, by Mr J. M. Way, in rocks which up to that time had been considered to belong in the Catskill formation or old red sandstone as it was frequently termed. This discovery was published in the latter part of 1862 by both Prof. Hall and Col. Jewett. In the autumn of that year Prof. Hall examined the rocks of this region in company with Prof. Edward Orton and Mr Way and published an article on its geology* which contained “a section from the north side of a Canadian naturalist and geologist, Oct. 1862, 7: 377. 118 - NEW YORK STATE MUSEUM the Susquehanna river to the high hills in the south part of Frank- = lin.” In this section Prof. Hall reported “ greenish and gray shales and shaly sandstone” as succeeding the Hamilton, then from 400 to 500 feet of “red shale and shaly sandstone with — numerous fucoidal remains ” which is now known as the Oneonta formation; while succeeding the red shales are about 100 feet of “ non-fossiliferous shale and shaly sandstone.” The greenish, red, and non-fossiliferous shales and sandstones or numbers 9, 8, — and 7 of the section were said to “ represent the Portage group.” The succeeding 250 to 300 feet of greenish to gray sandstones and shales are stated to contain fossiliferous bands in which are the bones and teeth of fishes associated with Brachiopod and Lamellibranch shells. Among the shells Spirifer mesastrialts ee Hall and Cypricardites chemungensis Vanuxem [Goniophora che- mungensis (Van.) Hall] were mentioned. Capping the hiils are from 100 to 150 feet of “greenish gray sandstones and shaly sand- stones’ in which fossils were not distinctly mentioned. In correlating these upper members of the section Prof. Hall said they “are always marked by characteristic fossils of the Chemung — group ” and that “ having... personally examined the region in “question, I do not hesitate to say that we have in the fossil re- mains taken together the most unequivocal evidence of the occur- rence of the Chemung group in these localities.” Col. Jewett reported that at Franklin he “found Mr J. M. Way, a gentleman ~ who for years has been examining the rock and collecting the fossils; and... he has succeeded in investigating the whole strata of the neighborhood and collecting many fossils. With his assistance I was able to make a section from the Ouleout creek to the top of a hill about three miles southwest of the village of Franklin, more than 800 feet in thickness,”” Jewett reported about 400 feet of red shale with some red sandstone at the base of this section above which was greenish shales and gray sandstones extending to the top of the hill, the upper 350 feet of which he reported as containing fossils of the Chemung formation to which he referred these rocks stating that he be- — lieved “that there is no’ old red sandstone (Catskill formation) — in this state.” a 15th an, rep’t regents on state cabinet of natural history, p. 198. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 119 In Prof. Hall’s address before the National academy of science in 1880 he again referred to the correlation of the rocks in Frank- lin,? and apparently referred the highest rocks of that township to the Catskill formation. Prof. Hall said “ crossing from One- onta and approaching Franklin over red and mottled shales and sandstones with an’ apparently southwest dip, these were suc- ceeded by gray and greenish shales and sandstones carrying Chemung fossils; and again on the road to Delhi these latter were succeeded by red rocks . . . The fossiliferous beds of the Chemung are found lying upon that formation [the Oneonta] between Norwich and Oneonta, and to the east of Sidney Plains [Sidney], and at or near Franklin, where they apparently pass _ beneath the great red sandstone formation of the Catskills, which is characterized by the presence of bones and scales of Holop- tychius.”’ | Darton, in considering the “stratigraphic relations of the Oneonta and Chemung formations in eastern central New York,” reported that ‘‘ The fossiliferous Chemung shales overlying the Oneonta formation south of Franklin have a thickness of about 800 feet and present the usual Chemung character. They grade upward through a series of flags, into hard, coarse, crossbedded - gray sandstones with intercalated red shale layers.’ While in Franklin the writer called upon the widow of Mr Way who was killed in the civil war, and she informed him that Round Top hill was one of his best localities for collecting speci- mens. Another place described to me by Mr E. P. Howe of Frank- lin, who was well acquainted with Mr Way, is on the western side of Ouleout brook opposite the Franklin mills between 8&0 and 90 feet above the level of the creek. At this locality there is a ledge of reddish sandstone over thin, gray sandstone and Mr Howe thinks the fossils came from the red rock. There is no question but that this zone is in the upper part of the One- onta formation. Mr Howe found in grayish sandstone, probably near the base of the Oneonta formation, a fine specimen of Arche- opteris jacksont Dn, near the foot of the northern slope of the } @Seience, old series, Dec. 11, 1880, 1:290. b Am. jour. science, 3d ser., 1893, 45:1207. gS ya, So Gee a ee eae meat) nba 120 NEW YORK STATE MUSEUM hill between Franklin and Otego in Otego township. ‘The speci- men now belongs to the museum of the State university of Ohio— | and has been kindly loaned by Prof. Edward Orton for the fig- fay ure which appears in this report. LXVI A. In the eastern part of Franklin on the southern fork. of Ouleout brook is the small village of Treadwell (formerly Croton). To the south of the village is the valley of Roaring brook and a | section of 350 feet was studied leading up this valley and toward eet _ the summit of the hill on the western side. Directly south of Treadwell on the western side of Roaring brook is an exposure of some 10 feet of red sandstone (A?) perhaps about 25 feet above oat the center of the village. This outcrop is in the upper part of the Oneonta sandstone as is shown on the Geologic map of New York. For 130 feet on the side of the hill the rocks are covered, then a ledge of thin bedded gray sandstone two feet thick (A*) occurs. The rocks are then mostly covered for 88 feet when the base of the Prime quarry is reached. However, about 15 feet below its base but farther to the east is a ledge of slightly red- dish sandstone. Perhaps the reddish color is due to weathering” and it may be considerably above the top of the Oneonta. The rocks are so well covered that on the lower slope of this hill the line of division between the Oneonta and Chemung was not de- termined. The Prime quarry (A‘°) is on the hill about three quarters of a mile south of Treadwell and some 255 feet higher. In the wall of the quarry 13 feet of rocks are shown, the lower eight feet being fairly fine grained, greenish gray flagging stone _ which splits into flags from two to three inches in thickness. In ~ the debris of the quarry and loose on the hillside are numerous blocks of stone containing large numbers of Crinoid segments. Such a layer filled with these segments occurs near the top of the sandstone. The upper five feet of the quarry is composed ~ mainly of greenish argillaceous shales in which are a few coarser layers containing numerous Crinoid segments. In addition to these a specimen of Tentaculites spiculus Hall (?) and another of Orthonota (2?) parvula Hall were found. The rocks forming this quarry are considered to belong in the lower part of the Che- mung. 42 feet above the top of the quarry is a five-foot ledge ~~ " Plate ¢ WINKOGr aL LE! ARCHAEOPTERIS JACKSONI Datoson Oneonta sandstone, Otego, N. Y. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 121 (A8) of similar greenish sandstore which thickens toward the top, while 30 feet higher is a four-foot ledge (A) of thin bedded, grayish sandstone which is the highest outcrop examined on the - hill. 349’ 345’ 165’ 35’ 0’ TREADWELL SECTION LXVI A A?° Thin bedded grayish sandstone A® Covered A* Greenish sandstone A” Covered A® Prime quarry. Sandstone and shale 250 (¢) slightly reddish sandstone A® Mostly covered A* Thin bedded gray sandstone A? Covered | = A? Red sandstone A! Covered Center of Treadwell 122 NEW YORK STATE MUSEUM . ty Darton compared the Chemung section south of Franklin with — that at Treadwell (Croton) stating that in tracing the fossilifer- Pig ous shales of the Chemung eastward from Franklin “they were found to gradually merge into flags and then into harder, coarse sandstones till at Croton, 10 miles east, their horizon is repre- sented by a heavy mass of coarse, gray, crossbedded sandstones eon with flaggy layers.’ . Near the township line between Franklin and Meredith and just below West Meredith are ledges of red shale and sandstone | oF. on the hillside a little south of the road. This outcrop is about 55 feet above the corners at West Meredith. Another ledge of _ thin bedded, red sandstone 30 feet in thickness occurs 55 feet — higher and this is capped by similar thin bedded gray sandstone. These rocks apparently belong in the Oneonta sandstone and are near the line of division between it and the Chemung as mapped on the Geologic map of New York. On a loose block of greenish Chemung sandstone a good specimen of Schizodus chemungensis (Con.) Hall was found and in the red sandstone a good specimen of a branching algoid plant. Toward the divide southeast of West Meredith and 215 feet higher is a coarse, massive greenish ~ sandstone which as represented on the Geologic map of New York — is probably in the Chemung. | When the sections of the rocks overlying the Oneonta sand- stone at West Meredith, Treadwell and Franklin are compared with the synchronous deposits on the Susquehanna river at Bain- bridge and Afton, the far greater amount of coarse grained sand- — stone is at once noticed. The shales and somewhat calcareous, fossiliferous layers of the Susquehanna valley Chemung seem to ey ‘ have largely disappeared and to have been replaced by these coarse sandstones. This change is still more marked to the east- ward in the drainage area of the Delaware river as will be seen in the description of that region. Delaware valley To the south of Franklin and the western part of Meredith township the drainage is southerly into the Delaware river. On a Am, jour. science, 3d ser., 45: 207. CLASSIFICATION, ETC. OF HAMILTON-AND CHEMUNG SERIES 123 account of the comparatively small number of sections of suffi- cient importance to merit a description, as wellasthemonotonous repetition of red sandstones and shales alternating with coarse, greenish gray sandstones, it is considered best to describe this | region under the general heading of the Delaware valley. LXV D+. In the southwestern part of Meredith township about five miles northwest of Delhi and barometrically 720 feet above the level of the Delhi postoffice is a small, glacial lake known as Spring lake or Robinson’s pond. This lake which is the source — of one branch of Steel’s brook, a stream lined along the lower part of its course by steep hills, is well toward the top of the highest hills and flows southeasterly and enters the Delaware river at Delhi. Just above the lake are thin bedded greenish sandstones which have the finer lithologic structure of the Chemung rather than that of the coarse grained sandstones of the Catskill formation to the east of the Delaware river. Alter- nating with these sandstones there are thin, greenish, arenaceous — shales similar to those of the Chemung formation. There is also, below the highway, a ledge of thin bedded, faintly reddish sandstone which is apparently replacing the greenish gray, colored sandstones of the Chemung. This stratum if followed to the west probably changes to a typical Chemung sandstone, while to the southeast of the Delaware river it becomes a red sandstone with the lithologic appearance of those of the typical Catskill. This gradual merging of the structural char- acters of the Chemung with those of the Catskill was clearly stated by Darton and shown in the figures illustrating his paper. He also says that the Chemung formation is “ overlain by several thousand feet of hard, coarse, crossbedded gray sandstones with intercalated red shales and gray flags into which they merge eastward and at the expense of which they expand westward. ° This merging was studied with great care-and it was found that stratigraphic continuity throughout is beyond question There is no overlap or wedging out of the beds either as a whole or singly but a gradual transition of coarse materials into fine materials. Lower and lower shaly beds are successively involved eastward till at a point about due south of Oneonta the lowest : : 3 are pee eee oe ae pe Fe ‘ é 1 * 2 "s ey aie « 128 gc Rout NEW YORK STATE MUSEUM Se eres = beds of shale finally merge into hard, coarse grained, cross : bedded gray sandstones.’@ Sey CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 131 but we were not fortunate enough to find any in place although some were found loose along the tributaries of the Delaware be- low this village. _ Along the lower course of the Holmes Hollow brook, one mile above Delancey, in the eastern part of Hamden and western part of Delhi townships are loose pieces of bluish shales containing some fossils as Liorhynchus, large and small Crinoid stems and an occasional other specimen. Some rather calcareous pieces — contain very poorly preserved specimens of a-large Spirifer. The list is: . 1 Chonetes scitula Hall 2 Liorhynchus mesacostalis Hall 3 Orthoceras sp. These loose pieces may be from ledges along this valley and of Chemung age. They are hardly rounded enough to have been transported any considerable distance by water. Unfortunately, the slopes of the steep hills lining this narrow valley are covered by drift almost to their tops so that there is not much opportu- nity to hunt for these fossiliferous shales in place. On the northern side of the brook near the western line of Delhi town- ship, about 400 feet higher than the river road is a thin bedded, ~~ coarse grained grayish to greenish gray sandstone, (LX VB?) with an exposure of 16 feet. In the field below these ledges are large blocks of loose reddish sandstone. Then about 75 feet are coy- ered when another ledge of thin bedded gray sandstone 29 feet thick is reached. Above for 45 feet it is apparently red shale - mostly covered and this is capped by a ledge of gray sandstone some 25 feet in thickness. For the next 70 feet the rocks are covered, then a ledge of thin bedded, gray sandstone five feet thick occurs near the summit of the hill on which are numerous blocks of unworn red sandstone. The rocks just described forming the upper part of this hill are represented on the Geologic map of New York as in the Chemung formation but their texture and general lithologic appearance are similar to those of the lower part of the Catskill formation in the eastern part of Delaware county. This section may be represented by the fol- lowing diagram: . "SECTION OF HOLMES: > HoTLOW BROOK ny Ey joke! hae be Near summit of hill Ay 5’ | Thin bedded gray sandstone 1m Loose blocks of red sandstone ’ 40’ | Covered | ED: aR iat 5 . Joe 90" ce eee 8d 25’ Gray sandstone y ‘ 4 ah 45 B: Red shale, mostly covered 29’ | Thin bedded gray sandstone , 75’ | Covered 16’ | Greenish gray to gray sandstone Ci | Loose blocks of red sandstone 400’ | Bt Gavered: Chemung (?) 0’ |———| Delaware valley road > ‘CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 133 Along Bagley’s brook east of Delancey (formerly Lansingville) a few fossils were found in loose pieces of shale similar to those in the Holmes Hollow brook: Spirifer mucronatus Con. fat 2 8. mesastrialis Hall 3 Sphenotus contractus Hall 4 Microdon (Cypricardella) tenuistriatus Hall The lower slopes of the hills along this stream are also covered by soil, drift and gravel so that there is no opportunity to ex- - amine the bed rocks. Higher in the hills are red and gray sand- stones and shales. es | LXV A. On the eastern side of the Delaware river to the north- east of Delhi is a steep hill known as Federal Hill. Along the Federal Hill road from the Delaware valley road nearly to its summit are frequent ledges of red sandstone and shales alter- nating with grayish sandstones. Near the summit of the road is more of the gray sandstone below which the rocks are prevail- ingly red. In the field on the south side of the road, about 65 feet above the base of the coarse gray sandstone exposed on the road near its summit, is the top of a ledge of thick, gray sand- stone. However, there is a zone of red between the top and bottom of this mass of gray sandstone. On the Geologic map of — New York the Oneonta sandstone is represented well toward the summit of Federal Hill, which is apparently correct, but its top is mapped as capped by Chemung. ! On the hill south of the Delaware river in the western edge of Stamford township, opposite Bloomville, are quite thick ledges of sandstone near the boundary line between the Oneonta and Chemung formations as represented on the Geologic map of New York. ‘First there are ledges of about 40 feet of greenish gray, coarse grained sandstone. In the lower part of these sandstones are specimens of Rhodea pinnata Dn., which are common in one place. Succeeding the gray sandstones are those that are red- dish and thin bedded, at least 35 feet thick with a layer of gray sandstone about 20 feet above their base. Then the rocks are 134 NEW YORK STATE MUSEUM covered for about 14 feet when a ledge of massive, quite thick bedded, gray sandstone, from eight to 10 feet thick, occurs and this is capped by red sandstone. With the exception of the plants no fossils were found, and the rocks more nearly resemble the Oneonta. or Catskill than the Chemung. On the hill te the south of Almeda, a station about half way between Hobart and Bloomville on the Ulster and Delaware rail- road there is, for about 80 feet from the railroad, for the most part soft, argillaceous shale; then a ledge of coarse, greenish gray sandstone is reached which is about 35 feet thick. Above, the rocks are partly covered, but there are quite frequent ex- posures of red shales and: sandstones which extend nearly to the top of the hill, 180 feet higher. The top of this hill to the north of Rose’s brook is apparently in the Chemung formation as colored on the Geologic map of New York. Again, the dividing line between the Oneonta and Chemung is represented as run- ning near the clove road south of Hobart. On this road near the head of the clove is a bank of soft red shale 10 feet in thick- ness. On the clove road and bank of the brook some 180 feet lower than the red shales are coarse, grayish, irregular bedded sandstones between red shales. The upper part of the ledge is coarse grained red sandstone with the same texture as the gray sandstone. There are layers of breccia with clay pebbles, slightly calcareous, but no fossils were found. There is so much red shale in this vicinity that the roads and fields are colored red from it and it makes a fertile country. These outcrops south of Almeda in Stamford township and along the clove road seem to be in the Oneonta sandstone. Roxbury To the east of Stamford township and the upper valley of the ~ Delaware river is Roxbury, the most eastern township of Dela- ware county. It is crossed from the north to the south by the east or Pepacton branch of the Delaware river which is lined on both sides by steep hills or mountains. On the Geologic map of New York the river valley and the lower slopes of the hills are VARWIV 10 HLNOS ‘UAAIN GUVMVIAG AHL GUVMOL ARTIVA MOOUM ASOYU NMOG META OI CHOAMW YO HOSANNA TIWH dOOMN AM Py 9}"1d CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 135 represented as in the Oneonta sandstone, while the higher part of the hills igs colored as in the Chemung formation. There are fair outcrops along the highways crossing these hills, both to the east and to the west of the river, which afford a ready means for comparison between them and the Chemung rocks in the western part of Delaware county and along the Susquehanna valley. LXIV D. One of the best section noted for such comparison is the one along the Roxbury and Hobart highway across the high hill to the northwest of Roxbury. This section is shown diagram- matically in another part of this report; but it is of sufficient im- portance to merit a more detailed description. From the bridge level over the east branch of the Delaware at Hubbell corners for some 73 feet the rocks are covered; but where the road forks for Hobart and Bloomville, and lower toward the brook there is an outcrop (D’) of 27 feet of red argillaceous shale. On the Geologic map of New York the line of separation between the’ Oneonta sandstone and Chemung formation is represented as crossing the road at this fork. From this fork to the summit of the hill on the road is barometrically 880 feet, and along the highway there are numerous outcrops of red sandstone and shale alternating with gray sandstone; also layers of breccia both red and greenish gray in color containing fragments of fish bones. On the hill south of the highway and 70 feet above the road Summit are ledges of gray and red thin bedded sandstones some of which have very much crossbedded structure. On the Geologic map of New York the rocks from the Bloomville-Hobart fork up to the summit and down the western divide are colored as in the Chemung, while the base of the Catskill is represented near the top of the high hill south of the road summit. This would give at least a thickness of 900 feet for the Chemung on this hill. In this section it is difficult to recognize any of the characters of the Chemung of the western part of Delaware county and apparently, about the same lithologic characters ex- tend from the Oneonta sandstone along the river valley to the top of the high hill, and it seems to the writer that the conditions _ under which the Catskill was deposited have about replaced those of the Chemung. ae a in age than the Cuuae far a is : nerfeetly evident tig bh Sy ene Met least the lower part of the formation and perhaps all } , (ie he if synchronous with the Chemung as found farther west in s ) ip re, ‘ail York. There can be no question but that the Chem a a of ved and ae sandstones, shales, and conelomerees. found shay _ the Catskill mountain region and is used in this sense ~ Present oe a8 was s crossed The section is along the first east road south of on Ny SECTION SOUTHEAST OF ROXBURY quai C® 465’ |———| Red shales on summit of road oe a a 725’ Block of red shale on road oe MT Ce ) 595’ | 170’ | Covered ; Red and gray sandstones and shales ty . 3 Partly covered pon 2950 100) | Ce te ; Mostly covered Sa a et ee a Ooh hf Greenish gray coarse sandstone a ' and reddish sandstone . 115’ * Covered rh 4 oy of river road, ae 50 feet above the river — 0’ |——— A hee The lowest ledge in the above section (C2) shows large blocks oe of coarse, greenish gray and red sandstone some of which are elle | | his rat Sah pin oe oY. 7 is Se es | Se ae ae hy fa Ce ES Ye Nt Mia 2 Pi pam a. ee % ear 1 SY ha) > at x yf CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 137 in place and others not. There are layers of breccia with clay pebbles but no fossils were found. In C! there are red: shales below, then coarse grained gray sandstone which is reddish — above, and the upper 45 feet as far as exposed is red sandstone. There are algoid stems in the coarse red shale but no other fossils were found. The upper part of the hill (C‘) is apparently all red argillaceous shale, some of which is of blocky structure, showing on the main Roxbury road about 40 feet below the summit of the hill: On the Geologic map of New York the Oneonta sandstone is represented along the lower part of the hill while above this and reaching its summit is the Chemung formation. As is seen from the above section in the upper 270 feet of the hill red shales and sandstones apparently. predominate. Through the pass between Roxbury and Grand Gorge the coarse greenish gray sandstones, and red shales and ee. of the Oneonta formation are well shown. On the hill about one mile north of Grand Gorge (formerly Moresyille) on the northern side of the Bear kill in the southern part of Gilboa township, is the following section in the Oneonta sandstone. _ SECTION NORTH OF GRAND GORGE LXIV B 320’ {———| Top of hill 35’ | B* Gray coarse bedded sandstones forming a massive ledge 10 feet thick at the base 285’ |——— ral Sean be 9 Gerda 265’ |——— 40’ | B’ Thin bedded grayish sandstone, irregularly bed- ee a ded and forms massive ledge 225’ | B1 Gray sandstones and shales alternating with red to creek level. Partly covered Goh ct Level of the Bear kil! ef Nae 138 NEW YORK STATE MUSEUM No fossils were found in the above section or in any of the ex- posures examined in the vicinity of Grand Gorge. The red — | - shales and sandstones of the Oneonta are conspicuous in the hill southwest of Grand Gorge and the rocks in the vicinity, of the village are represented on the New York map as near the middle of the formation which according to the generally understood limits of the Oneonta formation seems to be about their strati- - graphic position. CHARLOTTE VALLEY SECTION The Charlotte river rises in the northwestern part of Summit township, Schoharie co., and flows generally in a southwest- erly direction across the northern part of Delaware co., enter- ing the Susquehanna river at Emmons, above Oneonta. To the north of the river is a steep range of hills across the southeastern part of Otsego co. | separating its valley from that of Schenevus creek, while to the south is a wider divide between the Charlotte and Delaware river valleys. The rocks along the immediate river valley belong mainly in the Ithaca formation — while part of the steep hill to the north is capped by the Oneonta formation which forms, very largely, the northern slope of the - hill on the south. | 3 Davenport Davenport is one of the northern tier of townships in Dela- ware co. bounded on the north by Maryland and Oneonta township of Otsego co., and on the west by Franklin. The Charlotte river crosses the township from its eastern border nearly to its western line and receives a number of branches; the larger ones from the south. The slopes of the hills are pretty well mantled with drift, and no very extensive sections were discovered during the hasty examination which it was pos- sible to give the township. In general, however, it was deter- mined that along the river valley the rocks belong in the Ithaca formation; while the upper part of the steep: hill to the north along the Davenport-Maryland township line is capped by the Oneonta which extends considerably farther northeast than is represented on the Geologic map of New York. NOLSGNVS AVUD VLINOHNO ‘SsSvd GH)HOH GNVUD Ao GNH LSHM FHL IV Maia CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 139 On the hill north of the Charlotte river, northeast of Davenport Center, at an elevation of some 166 feet above the river level are ledges of bluish shales (LX XII C’) containing Ithaca fossils. About 60 feet higher are large, loose blocks of the Oneonta sandstone which caps the hill and have probably rolled down from it. On the north side of the river, about three fourths of a mile north- east of Davenport, almost opposite the mouth of Middle brook, and nearly 70 feet above the river road are ledges of bluish shales (LX XII A’) in the Ithaca formation from which the follow- ing four species were obtained as the result of a few minutes search: 1 Actinopteria boydi (Con.) Hall (a) 2 Chonetes setigera Hall : (as 3 Camarotoechia stevensi (Hall) H. & C. (?) (rr) Imperfectly preserved. 4 Phacops rana (Green) Hall | | (rr) One fourth of a mile northeast of Fergusonville, by the side of the highway, there is an exposure of 15 feet of bluish shales and sandstone (LX XIIB?*). The rocks belong in the Ithaca formation; but are not very fossiliferous. Specimens of Liorhynchus mesacos- talis Hall and Microdon (Cypricardella) gregarius Hall were obtained. Along a small brook, a northern branch of Middle brook, in the northeastern corner of Kortright township about three miles southeast of Davenport, are bluish shaly sandstones pe A?) containing fossils. Those found were: | 1 Spirifer mesastrialis (Hall) | (c) 28. mucronatus (Con.) Bill. (c) 3 Tropidoleptus carinatus (Con.) Hall (rr) The outcrop is perhaps one half mile above the valley road along Middle brook and the rocks are in the Ithaca formation. _ The hill to the north of Middle brook in the northeastern corner of Kortright and southeastern corner of Davenport was ex- amined, some 385 feet higher, near its summit and the general elevation of the highest land of that region. Toward the upper =. TAO? vue NEW YORK STATE MUSEUM part of the hill only ledges of gray, thin bedded sandstone es were seen in place. Some of the grayish sandstone shows fine examples of oblique bedding. Near the top of the hill — part of the sandstone is of greenish gray color and a specimen was found containing Amnigenia catskillensis (Van.) Hall, which . apparently came from one of the greenish layers. On the surface is an abundance of loose, red rock which must have formerly | capped the hill, but none was found in place. Mr Fisher has given some time to the study of the geology of the southern part | of Davenport and he has kindly contributed the following notes: The townships of Davenport and Harpersfield form the extreme northeastern portion of Delaware county. The country is hilly, . but the hills are neither so high nor so steep as those in the more central and eastern part of the county. They are drained by the Charlotte river and its branches, the river itself being a tributary of the Susquehanna. The low ground in the valley of the Charlotte, and the bases of the hills on either side of it, are made up of rocks of the Ithaca formation. The tops of the hills are capped with the heavy — sandstones of the Oneonta formation. | The lower part of the valley, between West Davenport and Davenport Center, was searched pretty carefully, but very few exposures of rock in place were found. The country is very . largely covered with drift and soil, so that even the deeper cuts along the line of the Cooperstown ae Charlotte Valley railroad expose only thick beds of sand and coarse gravel. The loose stones found along the roadsides and in the bed of the creek, which are greenish gray shales and soft gray or brown sandstone, are very fossiliferous, and from these loose pieces the following Ithaca — fossils were collected. 1 Nucula corbuliformis Hall 2 Nuculites oblongatus (Con.) Hall 3 Palaeoneilo plana Hall 4 Palaeoneilo emarginata (Con.) Hall 5 Palaeoneilo muta Hall 6 Palaeoneilo maxima (Con.) Hall 7 Microdon (Cypricardella) bellistriatus Con. 8 Microdon (Cypricardella) gregarius Hall 9 Macrodon hamiltoniae (?) Hall 10 Modiomorpha mytiloides Con. 11 Grammysia sp. 12 Paracyclas lirata (Con.) Hall 13 Glyptodesma erectum (Con.) Hall CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 141 14 Leptodesma rogersi Hall 15 Actinopteria boydi Hall 16 Pleurotomaria luca Hall 17 Spirifer mucronatus Con. 18 Spirifer mesastrialis Hall 19 Spirifer tullius Hall 20 Spirifer medialis Hall 21 Chonetes coronata Con. 22 Tropidoleptus carinatus Hall 23 Camarotoechia contracta (Hall) H. & C. 24 Crinoid segments | | On the north side of the river the only exposure that was found was one ledge of coarse gray sandstone, 17 feet in thickness, near . the top of the hill about one mile east of Davenport Center. In ' this ledge the sandstone is thin bedded, somewhat diagonally stratified and presents all the features of the typical Oneonta, which is certainly found on the higher part of this ridge of hills. On the south side of the river the results were a little more satisfactory. Near West Davenport, in a small depression by the roadside, were found some large angular blocks of a soft gray sandstone containing a few fragments of shells. On the hillside, about half way between West Davenport and Davenport Center, is a long low ledge of coarse gray sandstone. This ledge, which is 15 feet in thickness and is situated about 70 or 80 feet above the bed of the river, runs along the face of the hill for a consider- able distance. No fossils whatever were found in this rock, which fact, together with its lithologic character, a very coarse, thin bedded, gray sandstone, leads to its classification under the Oneonta formation. From the position of this ledge so near the bottom of the hill, it would seem very probable that it marks the line between the Oneonta and the softer rock of the Ithaca, which has all been worn away and covered by drift. In the upper part of a small brook which flows into the Charlotte about one half mile below Davenport Center, is an ex- posure of about 30 feet of heavy red sandstone. This rock forms a series of low falls in the brook just below an old mill dam. This exposure, both from the character and color of the rock, and from its position near the upper part of the hill is very certainly Oneonta. ; WILLIAM L. FISHER Worcester é Worcester is the southeastern township of Otsego co., with Maryland on the west, Westford and Decatur on the north, Sum- mit township of Schoharie county on the east, and Harpersfield 142 NEW YORK STATE MUSEUM township of Delaware county on the south from which it is. 7 * : separated by the Charlotte river. The Schenevus creek crosses the northern part forming a narrow valley lined by steep hills and in the southern part is the broader valley of the Charlotte : river which receives a number of tributaries from the north. ‘Separating the two valleys is a steep and high ridge which ex- tends southwesterly across the southern part of Maryland and : the northern part of Davenport and into the eastern part of Oneonta and southern part of Milford nearly to the junction of the Charlotte and Susquehanna rivers. The upper part of this high ridge from its southwestern end northeasterly into the western part of Worcester is composed of the massive greenish — gray sandstones of the Oneonta formation. This was so repre- — sented on the geologic map published in part 1 of this report; while on the Geologic map of New York the Oneonta formation was mapped as occurring only near the summit of the ridge | which it followed for about four miles along the Millford-Oneonta and Maryland-Davenport township lines into the western part of the last two townships. There are conspicuous exposures of the massive Oneonta sandstone on the hill south of Schenevyus in the southern part of Maryland which were briefly described in the former report®. On the hill to the east of the schoolhouse are heavy ledges of the greenish gray sandstone which form typical outcrops of the Oneonta sandstone and there are fre- quent outcrops of it along this hill to the east. By the high- way a little over two miles southeast of Schenevus, red sand- — stones are exposed below the gray sandstones. This locality is near the Maryland-Worcester line and about 100 feet higher than the base of the Oneonta sandstone at XXIII‘, on the hill | south of Schenevus. The Oneonta sandstone extends along the ridge for rather more than a mile into Worcester township, being last seen on the high point near the first road which turns to the south. XXVIA®. On the top of the steep hill one and one half miles south of Worcester and 800 feet above the railroad station at a 15th an. rep’t N. Y. state geologist, p. 268, 22 I+. + CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 143 Worcester are blue shales containing the Ithaca fauna, Spirifer mesastrialis Hall being common, and the upper part of this hill belongs in that formation. The following species were collected: 1 Spirifer mesastrialis Hall (r) _ 2 Palaeoneilo emarginata (Con.) Hall (?) (rr) 3 Microdon (Cypricardelia) gregarius Hall (c) 4 (?) Modiomorpha sp. | (rr) XX VI A2. Circumstances did not permit a careful examination for fossils in the rocks along the highway down into the valley; but some 390 feet lower than the horizon containing the Ithaca’ fossils are coarse, bluish, arenaceous shales with an abundant Hamilton fauna. The Hamilton rocks extend above the high- way corners where one road turns to the southwest and crosses Schenevus creek nearly two miles below the village. It was not determined whether this zone was about at the top of the Hamil- © ton or not but it is certain that there are over 400 feet of Hamil- ton rocks in the steep hill south of Schenevus creek at Worcester. In the few minutes spent in collecting at A? the following species were obtained: _ 1 Spirifer mucronatus (Con.) Bill. (r) 2 8. granosus (Con.) H. & C. (rr) 3 Tropidoleptus carinatus (Con.) Bill. (a) 4 Athyris spiriferoides (Eaton) Hall (rr) 5 Cramella hamiltoniae (Hall) H. & C. (?) | (rr) 6 Nucula bellastriata (Con.) Hall : (c) 7 Palaeoneilo constricta (Con.) Hall (rr) Bue; maxima (Con.) Hall (rr) That there was not the opportunity to make a thorough ecol- lection from the Hamilton rocks of this hillside is a matter of regret for it is apparently an excellent locality at which to obtain a characteristic fauna of the upper part of this formation. The general outline of the section may be represented by the follow- ing diagram: : 144 NEW YORK STATE MUSEUM SECTION OF THE HILL SOUTH OF WORCESTER AD). 9. aN BG. fa AS aed | A 390’ Partly covered Sherburne 7 20) SA 2) Hamelion fauna Partly covered 410’ | A’ Hamilton Q’ |——-—! R. R. level at Worcester On the hill south*‘of Schenevus creek two and one half miles about east of Worcester and 700 feet above the creek level is a thin, rather coarse grained sandstone quarry (26B!). A single specimen of an imperfectly preserved Lamellibranch shell was found belonging either to the genus Actimopteria or Liopteria. Still higher in the field are more argillaceous, non-fossiliferous shales and more argillaceous sandstones which together with the sandstones of the quarry belong in the Sherburne formation. The line of division between the Hamilton and Sherburne forma- tions may be followed along the side of the steep hill south of Schenevus creek nearly to the schoolhouse at the four corners in district no. 15, toward the head of Multer creek*, nearly two miles southwest of East Worcester. Then the line turns nearly to the south and follows the hill on the western side of Multer creek through Center valley, crossing it near the center of school district no. 18. The line next runs to the north and then south across the ridge east of Multer creek, makes a loop on the hill to a No name was found on the maps for the largest tributuary of the Charlotte river from the north between South Worcester and Charlotteville and the name Multer creek is proposed for it om account of the presence of several families of that name in the lower part of its valley. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 145 the north of Charlotteville in Summit township, Schoharie co., and crosses to the south side of the Charlotte river a little below the village and then continues along the side of the hill on the south side of the river northeasterly toward Summit village. XX VI B?. Along the highway in the upper part of Multer creek, district no. 15, about two miles Southwest of East Worcester are blue argillaceous shales containing Hamilton fossils and the | rocks belong in that formation. This exposure is only a short : distance above the road corners and the schoolhouse. The fol- lowing species were collected: 1 Tropidoleptus carinatus (Con.) Hall (a) 2 Vitulina pustulosa Hall 3 (a) 3 Spirifer mucronatus (Con.) Bill. BK Gg ke 4 Nucula corbuliformis Hall : : :. 2(@) 5 Nuculites triqueter Con. ae : (r). 6 Macrodon hamiltoniae Hall (rr) XXVIB%. On top of a high hill three fourths of a mile south of : East Worcester are blue argillaceous shales in the upper part of the Hamilton formation. This locality is about one and one half miles northeast of B? and approximately 240 feet higher. The fossils are as follows: 1 Spwrijfer granosus (Con.) H. & C. (rr) 2.8. mucronatus (Con.) Bill. (rr) 3 ON. tulluus Hall (?) . (rr) 4 Vitulina pustulosa Hall | (r) 2 Tropidoleptus carinatus (Con.) Hall | (Gc) 6 Nuculites triqueter Con. (rr) 7 Hyolithes aclis Hall ie (rr) XXVIB*. On the highway leading into East Worcester, 85 feet below B®, is a fair exposure of the blue argillaceous shales of the Hamilton which are quite fossiliferous, the following Species having been collected during a few moments’ search: 1 Spirifer mucronatus (Con.) Bill. (c) 2 Tropidoleptus carinatus (Con.) Bill. Pe a Ge (c) 3 Chonetes coronata (Con.) Hall Heelan a (c) 146 NEW YORK STATE MUSEUM 4 Nucula bellistriata (Con.) Hall : (c) 5 Nuculites triqueter Con. | | " (rr). 6 Palaeoneilo constricta (Con.) Hall - (rr) XXVI Ct On the hill west of Multer creek, about one and one half miles below Center Valley schoolhouse, is a small quarry in rather coarse grained, thin bedded, bluish sandstones similar to those on top of the hill south of Worcester and stratigraphically apparently in the Sherburne formation. This formation becomes more arenaceous as it is traced eastward and forms thin flags. Fossils are rare although the few found indicate the lower Ithaca formation to which, perhaps, these rocks should be referred rather than to the Sherburne. The list is: 1 Spirifer mucronatus (Con.) Bill. (r) 28. mesastrialis Hall (?) ae (rr) Broken and imperfectly preserved. 3 Tropidoleptus carinatus (Con.) Hall (rr) 4 Lamellibranch shell , (rr). 5 Fragments of wood XX VI C2. With the exception of some rather steep cliffs toward South Worcester the hill on the north side of the Charlotte river between South Worcester and the Multer valley is largely covered by soil. Rather more than one mile east of South Wor- cester near the top of the hill 450 feet above the river road are — loose, unfossiliferous, shaly sandstones, and some about in place that contain Ithaca fossils, as follows: 1 Spirifer mesastrialis Hall (?) (rr) Very imperfectly preserved. q 2 Microdon (Cypricardella) gregarius Hall (c) 3 Palaeoneilo plana Hall (rr) On the lower part of the steep hill about 90 feet above the highway nearer South Worcester is quite a prominent ledge of bluish shales. There are a few fossils, T'ropidoleptus carinatus | (Con.) Hall being the most abundant. This looks like the transi- tion zone from the Sherburne to the Ithaca formation. About Se, a eae = Se ae Se ke _‘. QOLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 147 100 feet higher on the hill are plenty of loose blocks, apparently from higher ledges, containing an Ithaca fauna. XXVID. On the western side of the brook valley, one and one half miles north of Charlotteville, or about four miles south of East Worcester is an interesting section in the upper Hamilton which follows the cross road west of the brook valley at the “First baptist church of Summit” and is near the township line between Summit and Worcester. About 107 feet above the level of the valley road by the side of the cross road are soft, blue, argil- laceous shales (D?) containing an abundance of Hamilton fossils. The list is as follows: 1 Spirifer mucronatus (Con.) Bill. (c) | 2 8. tullius Hall (rr) 3 ON. granulosus (Con.) H. & C. (?) (rr) - Very poorly preserved. 4 Tropidoleptus carinatus (Con.) Hall (r) 5 Leda rostellata (Con.) Hall (rr). 6 Schizodus appressus (con.) Hall. (rr) 7 Chonetes setigera Hall (rr) 8 Palaeoneilo maxima (Con.) Hall (r) 9 Nucula bellistriata (Con.) Hall (c) 10 Nucula corbuliformis Hall — (rr) 11 Nuculites oblongatus Con. About 50 feet higher is the Aaron Silvernaile quarry (D3) where some eight or nine feet of blue, flagging stone is shown. The sandstone splits into layers from one and one half to four inches in thickness and the quarry has been worked to a consider- able extent for flagging stone. Above the sandstone are shaly layers in which fossils are fairly common. The species listed below were collected on the dump heap of the quarry: 1 Spirifer tulius Hall | (a) Abundant in thin layers. 2 SV. mucronatus (Con.) Bill. (c) 3 8. Sp. (rr) Very poorly preserved; perhaps S. granulosus (Con.) H. & C. ite Tropidoteptus brain (Con) Halt) 2A 5 Glyptodesma erectum (Con.) Hall | 6 Grammysia bisulcata (Con.) Hall f t G. (Sphenomya) cuneata Hall ae 8 Modiomorpha subalata (Con.) Hall (?) - ae ig 9 Palaeoneilo constricta (Con.) Hall : ee 10 Pleurotomaria sulcomarginata Con. (?) DN ie a es clarkit, Sp. NOV. eee Fetheod 7 aoe f : Rt ine base of the Sherburne formation. A view of the pe Lah = ee ‘1 quarry ged another of the dump heap were given in par rt Lo vf SECTION OF HILL AT SILVERNAILE QUARRY oa Top of hill _ Sherburne (?) 55’ | D4 Covered ; : | 8 | D® Silvernaile quarry | oa eae Ee ee Hamilton | . on 50’ 107’ |_| D? Shales with Hamilton fossils 107’ | D* Covered 0’ |———| Level of;road in valley | as CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 149 ANNELIDA PLANOLITES Nicholson, 1873, Proc. Roy Soc., London, p. 289 Planolites clarkii nov. sp. Horizontal, tortuous, and undulating burrows or tracks which are simple, rounded furrows of about equal width throughout their length. One undulating track is 26 cm in length and 4 mm in breadth; while some of the very tortuous ones are con- siderably longer, as for example one is 59 cm and 5 mm in. breadth. The greater part of the burrows is not filled and is smooth. In the better preserved portions of some of the trails, however, are somewhat imperfect transverse parallel furrows and ridges, one specimen having 18 in the space of 1 cm. The ridges are broader than the furrows, varying from one half to three fourths of amm in width. These furrows and ridges apparently represent the segments of the worm. Other portions of the bur- rows are filled with. cylinders of arenaceous’ material, not especially different from the matrix, which have a smooth surface and show no structure. This filling is probably the sand that was passed through the alimentary canal of the worm, although it is possible that they are simply casts of trails as have been de- scribed by Nathorst. As far as noted these burrows were all in the lamination planes of flagstone strata. These tracks somewhat resemble Gyrichnites gaspensis White- aves? from the Lower Devonian (Gaspé sandstones) of Gaspé Bay, Quebec, but they are much smaller and not marked by the con- spicuous grooves of that species. A specimen was submitted to Prof. Whiteaves who wrote as follows: “Your specimen shows parts of the arenaceous filling of the burrow or mold, if it is an annelid track, and clearly differs from the Gaspé species of Gyrichnites, as you say, by its much smaller size. In your specimen, also, there seems to be somewhat greater rigidity, and a closer disposition of the transverse annu- lations. It is not at all easy to make up one’s mind as to whether your tracks should be regarded as referable to Planolites or to Gyrich- _ mites. For, although the convex filling of your specimen is no a Trans. roy. soc. Canada, sec. IV, 1882, p. 109, pl’s XI, XII. 150. NEW YORK STATE MUSEUM doubt scarcely distinguishable from Planolites, yet the concave Raa portion, into which it fits, is tranversely and closely annulated, as — it were, or at any rate shows transverse markings, a feature which is not indicated nor figured in Nicholson’s diagnosis and figure of Planolites. In this latter respect, no doubt, your specimens. " agree better with Gyrichnites, but they may, also, indicate a generic type different from either that genus or Planolites.” In regard to the transverse markings it is to be remembered that Planolites annularis Walcott from the Cambrian of Wasa ton co. N. Y., “shows numerous annulations.”@ The specimens might also be compared with Protoscolex ornatum Ulrich;® but that species has much shorter and slenderer tracks : with much narrower segments. Locality: Silvernaile quarry, Worcester township, four miles south of East Worcester and one and one half miles north of Charlotteville. Geological horizon: Near top of Hamilton formation. XXVIE*. On the valley road toward East Worcester and about one half mile north of the “ First baptist church of Summit ” are bluish, argillaceous shales containing plenty of fossils. This is a typical exposure of the soft Hamilton shales and the - following fossils were found: \ 1 Spirifer tullius Hall (rr) 2 Chonetes setigera Hall 3 (2?) Centronella impressa Hall (c) Imperfectly preserved and difficult to identify. | 4 Nucula bellistriata (Con.) Hall (a) Small form. | 5 Modiomorpha sp. (rr) 6 Leptodesma sp. : (rr) 7 Liopteria dekayit Hall ef (rr) 8 Murchisonia micula Hall (?) (rr) 9 Teniaculites bellulus Hall (c) 10 Crinoid segments (c) a See 10 an. rep’t U. S. geol. surv., p. 602, and pl. 60, fig. 5. bd Jour. Cincinnati soc. nat. hist., 1878. 1: 90, pl. 4, fig. 1. ess ne uy Se een es ay | WYNKGOP HALLENBECK CRAWFORDCO. PLANOLITES CLARKII Prosser Hamilton formation, Worcester, N. Y, CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 151 7 Summit Summit which is one of the western tier of townships in Scho- harie co. lies directly east of Worcester. The central part of it is an elevated plateau while in the western part are the upper valley and headwaters of the Charlotte river; in the northern part streams rise that flow northerly into the Cobleskill and in the eastern part streams that flow easterly into the Schoharie river. As has already been mentioned the line of division between the Hamilton and Sherburne formations crosses the Charlotte river near Charlotteville and follows the northern slope of the valley northeasterly to within, perhaps, one mile of Summit. Then it runs southeasterly along the Westkill into the northern part of Jefferson township where it crosses the stream and then turns northerly along the eastern side of the valley and around the high land east of Summit when it turns easterly and follows the northern slope of the hill south of Panther creek across the southern part of Fulton township into the Schoharie river region. XXVIX. To the south of Charlotteville and the Charlotte river is a steep hill rising nearly 600 feet above the level of the river, and in the banks below the dam at Charlotteville are blue flagging stones (X!) forming a ledge some eight feet thick. There are some layers containing plant stems and a few pebbles, and some partings of blue shale. The dip is about 1° S60° W. Along the banks of the river are plenty of loose stone containing Ham- ._ ilton fossils in abundance and the bed rocks resemble the flagging stones of the upper part of the Hamilton in the southwestern part of Albany co., to which formation this zone is referred. | For 400 feet above the river the hillside is covered when a ledge of massive bluish gray sandstone (X°) is reached southeast of Charlotteville. The stone splits into thin flags, in places is somewhat crossbedded and about five feet are shown. No fossils were found and it is apparently in the Sherburne formation. On the top of the hill southeast of Charlotteville 12 feet higher than X*, and near the Summit-Jefferson township line is a ledge | of thin, bluish sandstone to arenaceous shale (X5) containing fos- sils, specially Actinopteria boydi (Con.) Hall. The complete list is: 1 Actinopteria boydi (Con.) Hall fon (c) 2 Palaeoneilo emarginata (Con.) Hall var. . (rr) 3 Grummysia (Sphenomya) cuneata Hall (?) (rr) i Chaminien iohonene nents icon) Hall : #5 Spirifer mucronatus (Con.) Bill. (2) : a Coane eons sp. SECTION OF HILL SOUTH OF CHARLOTTEVILLE RONG sli XE ——| Top of hill X7 Sandstone and shales on road hs ‘ { 50’ oe 537’ |_——_| X® Bluish fossiliferous shales. Ithaca | 199’ | X* Covered fe Hay : ae 5’ | X* Bluish gray sandstone. he Sherburne (?) 410" | Bek | 409 X? Covered ‘ §’ |——— s’ | X! Sandstone. Hamilton (2) 0’ |————_| Charlotte river level CLASSIFICATION, ETC. OF, HAMILTON AND CHEMUNG SERIES 153 To the east of the hill described above, is the former hamlet of Morseville in the northern part of Jefferson township on the highway from Summit to Jefferson. On the hill east of Morse- ville is coarse grained, massive sandstone very similar in general appearance to the heavy sandstone seen at the base of the One- onta sandstone along the valleys of the Susquehanna river and Schenevus creek. Farther south on the hill about two and one third miles west cf north of Jefferson village and some 225 feet higher are massive deposits of this coarse grained sandstone (XX VII A). As far ag the color and lithologic appearance of this stone are concerned it would be difficult to distinguish it from typical exposures of the Oneonta sandstone in Otsego and Dela- ware counties. These ledges, however, are not considered to be -stratigraphically as high as the base of the Oneonta sandstone in _the Susquehanna valley; but it is thought that similar lithologic _ conditions appear at a lower horizon in rocks which are synehro- nous with the upper part of the Ithaca formation of .Otsego co. Itis believed the record of the observations across Schoharie co. will show that the conditions under which the Oneonta sand- stone was deposited in Chenango, Otsego and Delaware counties occurred earlier and earlier as the formation is followed to the eastward till the Ithaca formation finally merged into the Oneonta. The change seems to have been about the same as the one described in Delaware county where the Chemung formation merges into the Catskill. XX VII Ct. About one and one fourth miles north of Morseville and two and one third miles southwest of Summit village in the southern part of Summit township is a conspicuous mound or _ circular hill. Its top is approximately 170 feet higher than the four corners at Summit and it is a conspicuous landmark when seen from the high land to the east of Summit as well as from other localities in Summit and Jefferson townships. The rocks © are pretty well covered on the mound, but there are some ex- posures of shales and shaly sandstones; while the slope is quite well covered with loose pieces that evidently came out of the hill. Spirifer mesastrialis Hall with a few other species are found and ~ 154 - NEW YORK STATE MUSEUM © a the rocks are evidently in the Ithaca formation. On the highway 3 not far from the northern foot of the mound just described are — bluish shales which break into very small pieces and alternate with thick bedded sandstones. No fossils were found and the rocks of this outcrop closely resemble those of the Sherburne ' formation. On the highway immediately to the north of Summit are bluish arenaceous shales—typical Hamilton—containing numerous fossils. The village is certainly situated on rocks of the Hamilton formation. A short distance to the northeast of it in a sort of basin cut out of Hamilton rocks is a small, very pretty, glacial lake, completely surrounded by fields and woods, which may very appropriately be called Summit lake. Its outlet forms one of the head branches of the Westkill. A view of the © lake from the high hill to the north is given on one of the plates. XXVIID. Two thirds of a mile to the north of Summit and Summit lake is a prominent somewhat circular hill which may be called Summit hill. From its summit a magnificent view in several directions may be had. To the south are the western Catskills of Delaware co.; to the southwest is the upper valley of the Charlotte river with its maze of hills and to the north and north- east is the valley of the Cobleskill lined by its steep hills. From this commanding position a clear idea of the irregular surface carved out of this plateau by the streams may be obtained. On the highway ~where the descent begins toward the Cobleskill at Richmondville are bluish arenaceous shales containing an abun- dent Hamilton fauna. From the highway a section was con- structed along the quarry road up the southern side of the hill. The first 100 feet are covered and then for a few feet there are smooth, bluish shales without fossils. At an elevation of 115 feet rather coarse, bluish, arenaceous shales begin (D?) resem- bling the Hamilton shales in all respects. There are 15 feet of these shales containing numerous specimens of Hamilton fossils. This zone is still in the Hamilton formation, although very near its summit. The complete list of species collected in D?* is as follows: : GHL OL STITIMSLVD AHL GNV FUVI LINWAS AO MAIA L 9}¥1d ee 4 2 =a onda’ ee ey CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 155 1 Tropidoleptus carinatus (Con.) Hall | (a) 2 Spirifer mucronatus (Con.) Bill. (c) 3 8. tullius Hall (c) 4 Chonetes setigera Hall (rr) 5 Orthis (Rhipidomella) vanuxemi Hall (rr) - 6 Camarotoechia congregata (Con.) Hall & Clarke (?) (rr) Broken specimen. 7 Microdon.(Cypricardella) gregarius Hall en as 8 Palaeoneilo muta Hall (rr) : ane constricta (Con.) Hall (rr) 10 Nucula corbuliformis Hall (rr) 11 N. bellistriata (Con.) Hall , ce 5 12 Nuculites oblongatus Con. (rr) ; 13 Cimitaria recurva (Con.) Hall (rr) 14 Grammysia bisuleata (Con.) Hall - (rr) 15 Goniophora hamiltonensis (Hall) Miller (?) (rr) 16 Lnopteria dekayi Hall (rr) 17 Pterinopecten vertumnus Hall (rr) 18 Dalmanites (Crypheus) boothi (Green) Hall (rr) 19 Loxonema sp. : (rr) Only one whorl; too imperfect for specific identification. Above zone D? are much finer shales (D*) which contain an , eeasional fossil and resemble considerably the Sherburne shales | of Schoharie co. After 20 feet of these shales, however, there is an abundantly fossiliferous stratum of the coarser Ham- ilton-like shales (D*) but a little more than a foot in thickness. Above and below D# are the fine, smooth shales containing only an occasional fossil. The fauna of D*‘ is: | 1 Tropidoleptus carinatus (Con.) Hall (a) 2 Vitulina pustulosa Hall (rr) 3 Spirifer cf. granulosus (Con.) H. & C. (r). ; Internal impressions too imperfect for specific identification. 4 Spirifer sp. (rr) 5 Chonetes scitula Hall (rr). 6 Athyris spiriferoides (Eaton) Hall 156 NEW YORK STATE MUSEUM a 7 Nuculites triqueter Con. | (rr) i 8 Nucula bellistriata (Con.) Hall (r) “ 9 Grammysia (Sphenomya) cuneata Hall | (c) 10 (?)Prothyris sp. : é (TEs 11 Liopieria dekayt Hall (rr) ee he 12 Pleurotomaria capillaria Con. | (rr) This is the highest zone of Hamilton fossils found on the hill and is considered to mark the top of the formation above which oer are the shales and sandstones of the Sherburne formation. Above the fossiliferous zone of D+, 39 feet of the smooth, bluish, argillaceous shales are shown along the quarry road. These { shales which weather to an olive tint and soon decompose into soil closely resemble in lithologic characters the Sherburne ‘Shales, to the base of which formation this zone is referred. The 3 rocks are then covered for 35 feet when the base of the McDonald | & Co’s flagstone quarry (D") is reached near the top of the hill. There are 12 feet of rather coarse grained, blue sandstone shown in the quarry wall, the upper three feet of which have shaly _ pertings. The stone is quarried for flagging though some of the layers are rather thick. The sandstone is covered by 38 feet of slightly olive and bluish argillaceous shales, (D’) at the western — end of the quarry and 381 feet at the eastern end, containing some thin layers of sandstone and all weather to a more or less brownish color. At one place on the floor of the quarry are fine ripple marks. Some time was spent in hunting for fossils over — the large amount of debris from the quarry but nothing save a few rather poorly preserved specimens of Lepidodendron and fragments of plant stems wasfound. From the top of the quarry to the summit of the hill is some 20 feet more, all of which is covered. On the top of the hill is a monument of the New York state topographical survey that is 2428 feet A. T. The highway was followed from the beginning of the descent to Richmondville and then to Warnerville which is near the top of the Onondaga limestone. Along the upper part of the hill — are numerous outcrops of Hamilton shales and it is a good locality at which to study the upper part of that formation. The 0 ac RA, } : - ed nae See oie eka hr | ee ea Pe 4 ae, -* ee ee oe * ‘ J oa : X te cr ah Sao 1 re “ ars) thy CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 157 _ barometer gave a difference of 1155 feet from the fossiliferous band D# to the bridge above the Hamilton gorge in Richmond- ville. To this can be added the 26 feet of coarse, arenaceous shales shown in the creek in Richmondville which will give at least 1231 feet for the Hamilton formation in the northern slope of Summit hill. This, undoubtedly, is not the entire thickness of the formation since the shales in the Richmondville gorge are _too coarse for the shales at the base of the Hamilton formation. From the base of the shales in the Richmondville gorge to the level of the Cobleskill is 45 feet, which is covered. The above section is a fairly accurate one, for the altitude of the Richmond- ville railroad station is 1174 feet A. T. and that of Summit hill 2428 feet, making a difference of 1254 feet between the station and the top of the hill; while the barometric section is 1276 feet © which is only 22 feet too great. From the Richmondville gorge to Warnerville there is a fall of 200 feet which makes at least a thickness of 1355 feet for the Hamilton and Marcellus formations, — without taking into consideration the dip which would increase the amount. The barometric section from the top of Summit hill to Warnerville is 1500 feet. This is not far from correct for the difference between the Cobleskill railroad station, near the same level as Warnerville, and the top of Summit hill is 1526 | feet. The diagrammatic form of the above section is given in an accompanying figure. LI A. The brook on which the Richmondville gorge, mentioned above, occurs rises in the northern part of Summit township and cuts a deep and narrow gorge on the northern slope of Summit hill known as Bear’s gulf. There are numerous exposures along this stream to the gulf, and the section given has been con- structed from the Cobleskill along this brook through Bear’s gulf and to the top of Summit hill. The total thickness of the section is not as accurate as the one already described, for it makes the difference between the Richmondville railroad station and the top of the hill 1340 feet, which is 86 feet too great. The “gulf” is a narrow glen bounded by steep walls composed largely of Hamil- ton sandstones or coarse, arenaceous shales, a general idea of 158 NEW YORK STATE MUSEUM — which is here given; at the top is a cascade also shown | wae % the plate, and at the top of that is adam. The land on the west- ern side of the gulf belongs to Mr William Harinahs and on the eastern side to Mr David Wilday. In part 2 of the magnificent | work on the Lamellibranchiata of New York a number of species . are credited to this locality and it is certainly a splendid place {fcr collecting. There are numerous large blocks in the stream which have fallen from the cliffs along the sides of the gulf and they are filled with excellent fossils. On the section A’ and A& are the exposures for Bear’s gulf, the lower 235 feet of which are composed largely of coarse arenaceous shales containing an abundance of fossils, while at their top is the base of the high cliff. The cliff is composed of shales with rather thick, very fossiliferous sandstones and it is 180 feet from its base to the | dam at the head of the gulf. Time did not permit a thorough search for fossils; but the following fauna was obtained from zones A’? and A8, 1 Spirifer mucronatus (Con.) Bill. (aa) The very mucronate forms. 28. granulosus (Con.) H. & C. | (c) 3S. _ tullius Hall (c):, 4 Tropidoleptus carinatus (Con.) Hall (a) 5 Liorhynchus multicosta Hall (a) 6 Camarotoechia congregata (Con.) H. & C. | (c) 7 Productella sp. (rr) Broken specimen. < ; 8 Grammysia magna Hall (c) 92G. - bisulcata (Con.) Hall 3 (r) 10 Glyptodesma erectum (Con.) Hall (rr) 11 Pterinea flabella (Con.) Hall (rr) 12 Microdon (Cypricardella) tenuistriatus Hall (rr) 13 Nyassa arguta Hall — (r) 14 N. subalata Hall ; (rr) 15 Palaeoneilo emarginata (Con.) Hall , (rr) 16 Liopteria dekayt Hall (?) (rr) 17 L. bigsbyi Hall C oi (Fr) 27D SECTION No SVA SECTION CO ae OF FROM S.SIDE OF BLARSGUS, SWUYYT HILL WAP NERVILLE. PICHMONOVILLE TO SUMMIT og, COVERED To TOP oe pie. 1480 Si6 wae srariow Cover eo ro re2 or with. OLIVE SHALES AT WESTERN ENDO or QUARAY ~ FLAGbING STONE. SWALes. FLAasTOwE auARAy. B45 oF OVA AY. SHERBURNE Mosrey co VEF EO Covereno. SMOOTH Beuss H_ABGILLACEOUS SHALES. SHERBURNE. CosAseR SHALES wy OF FOSS/LS, FINESHALE WITH OCCASIONAL FOSSILS. = Ly COARSE BLUSH SHALE WITH PLEN_ry o- FOSSILS. 1305p S| cyoorn wi AMILTON, SHALES WITHOUT FOSSILS. TH PLENTYy MW osre v-CovEREO /00| CoveER ED. 120. LEVEL OF FOAD AT OESCENT To 4 OaM AT 192 OF BEARS GULF ACA MONOVILLE, SHALES ANO SAVOSTONES WITH FOSSILS BASE OF 16H CLIFF IN GULF.” COARSE SHALES WITH PLENTY OF FOSSILS Foor oF Beans Cure l00§| PARTLY COVERED SALES AND SANDSTONES. PARTLY COVERED HAMILTON LAYER WITH ABUNDANT FOSSILS THIN-BEQQED BLVE SANDETONE. @LUISH BLOCKY SHALES WITH ABUNOANT FOSSILS UPPER DAM FINE BLUISH SHALES. Mier STREET B9106E Fice MONDVILLE CONCRET ION ARY SANDSTONE. STAEET BRIDEE R00 Covereo, Leve. of Costes tite CREE WAANERVILLE HOTEL, CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 159 18 Tentaculites bellulus Hall (c) 19 Camarotoechia prolifica (Hall) H. & C. (r) - 20 C. 7 sappho (Hall) H. & C. (rr) 21 Orthothetes chemungensis (Con.) H. & C. var. arctostriatus Hall — (rr) 22 Orthonota undulata (Con.) (r) 23 Orthoceras sp. | (rr) 24° Chonetes coronata (Con.) Hall 2 (aa) There are splendid specimens of the variety that was called Strophomena syrtalis Con. The next 117 feet above the dam at the head of the gulf on the western side of Summit hill is mostly covered when a zone of fine bluish to greenish shales is reached (A?) containing an occasional fossil as Spirifer mucronatus (Con.) Bill. This outcrop seems to be near that of zone XXVII D? of the section on the - southern side of the hill. From the base of A” to the floor of the | _ quarry is 108 feet, the greater part of which is covered on the western slope of the hill. The remainder of the section is the same as that described in section XX VII D. _ Emmons in describing the rocks near Summit referred the higher ones to the Chemung formation, stating that “At Summit in Schoharie county, in a deep gorge near the village, the Che- mung group occupies the upper part and the higher slopes adjacent to it, and also the hills above the village. As yet, - however, the fossils of the Chemung narrows are not common or numerous; and it seems to be established that the fossils of the Hamilton shales go up higher into the shales and flags, and occur nearer to the base of the Catskill division or Old Red sandstone, than at the west.” , | In the above quotation it is not quite clear which gorge is | meant, yet it is probable that its rocks are in the Hamilton instead of the Chemung formation. As already shown the hills to the north and northeast of Summit are capped by the Sher- burne formation, or Portage as called by Emmons, and those to the south by the Ithaca. ; 2 Agriculture of New York, 1846, 1:192, 160 ete Magee tr “NEW YORK “STATE MUSEUM Jefferson . : To the south of Summit is Jefferson, the southwestern ship of Schoharie co., which is bounded on the south Stamford and Harpersfield townships of Delaware 0. - on the west by Harpersfield and a bet of Summit. Across ‘¥ -taries of the Schoharie river. In the northern part of the to ‘ship to the east of Morseville and northwest of Jefferson are ledges of coarse grained, greenish gray sandstone similar to ie Oneonta, which have already been mentioned. pate XXVIT B?. To the north of Jefferson village and Middle brook Me 7 op are exposures of thin sandstones and arenaceous shales, with some very calcareous layers which are composed largely of Spivifer — mesastrialis Hall. These calcareous layers are called “fire stones” ey by the farmers and the loose pieces are picked up and used for ie _ arches. Some of the rocks were found in place at about the - game elevation as the central part of the village; but it is approx- ‘ ae imately 190 feet lower than the coarse, greenish gray sandstone on the hill two and one third miles west of north of Jefferson (XXVII A’). The most abundant fossil is Spirifer mesastrialis Ne Hall which occurs in the calcareous layers, but some of the arena- ceous shales contain specimens of a few species of el The complete list of specimens is as follows: . 1 Spirifer mesastrialis Hall 2 8. mucronatus (Con.) Bill. 3 Camarotoechia exima (Hall) H. & C. 4 Tropidoleptus carinatus (Con.) Hall 5 Microdon (Cypricardella) gregarius Hall / CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 161 6. WM. (Cypricardella) complanatus Hall (rr) 7 Modiomorpha mytiloides (Con.) Hall (?) (rr) 8 Palaeoneilo emarginata (Con.) Hall var. Ay Cr) 9 Nucula bellistriata (Con.) Hall (?) (r) IG. corbuliformis (Con.) Hall (?) (rr) 11 Goniophora cf. hamiltonensis (Hall) Miller (rr) 12 Leptodesma rogersi Hall (?) (r) 13 Actinopteria boydi (Con.) Hall - ; (r) 14 Tentaculites attenuatus Hall (?) (Cc) These fossils are believed to occur between 350 and 400 feet above coarse, greenish gray sandstones which cap the hill be- tween the Westkill and Mill creek to the west of North Blenheim in the Schoharie valley. The explanation is that the coarse sandstones with the facies of the Oneonta sandstone appear lower in the Schoharie valley than in the Charlotte and Susquehanna valleys. This replacement of the Ithaca formation by coarse, greenish gray and red sandstones in lithologic characters similar to those of the Oneonta sandstone is well shown along the Scho- harie valley and to the eastward. Mather in his report on the first geological district mentioned this locality north of Jefferson Academy, as Jefferson was then called. He wrote, “shells were seen in many places in the grits and gritty shales, between Summit and Jefferson Academy, . especially on the high grounds and on the tops of the hills. They are particularly abundant’ about one mile north of Jefferson Academy.”* He simply mentioned them under the Erie division of the rocks, which in his district included the Marcellus, Hamil- ton, Ithaca and Chemung groups without referring them to any formation. On the Geological map of New York published in 1844, all of Jefferson township, except the extreme northern portion, is colored as in the Catskill formation. This would make the heavy greenish sandstones near Morseville the base of the for- mation. The northern edge of Jefferson and the southern two thirds of Summit are colored as in the Portage and Chemung a Geology of New York. 1844. Pt1, p. 321. NEW YORK STATE MUSEUM 162 formations, the northern part be alee being incl uae in -_ Hamilton. ; BS . Emmons discussed the rocks at Jefferson to some extent u a me the heading of the “Catskill group,” though he apparently cor related them with the Chemung. He said, “ Near the village, we rf discovered the same fossils as those of Gilboa, namely, the a8 Oypricardia, Tentaculites, Orthis, ete. Besides the strata of — ait crushed vegetables and the diagonal stratification already men- iA tioned, Mr Hall has discovered a scale of the fish characteristic | : of the Old Red sandstone. In these discoveries we have the facts. er Which have settled the character and age of the rocks in the : a e southern part of Schoharie, Albany, and those of Greene and — Delaware counties. They form one series of rocks, which may ae be traced south, southwest and west, through the southern tier of counties; and as a few fossils of the Chemung narrows have _ v3 been found in Gilboa, we are able to connect the series with ie ge distant points . west. The Chemung group, which had been “f sm supposed to be confined to the southwestern counties, has been on oh proved, by the discovery of fossils, to occupy a place also at the base of the Catskill series. Of the Dipleura dekayt [H omalonotus pels dekayt|, Microdon bellistriata, Cypricardia angulata, the latter a is credited to Chemung narrows, while the two former are well ae known Hamilton fossils; these, with several others, occur 500 : feet above strata which have hitherto been regarded as belong- ey, ing exclusively to the Catskill series.’’# oe - XXVII BY. On the hill to the south of Jefferson and Middle brook is a prominent ledge of massive coarse gray to greenish pe : sandstone, with reddish sandstone at the top, which is about). b4 feet above the village hotel. This ledge in all its lithologic char- acters is like the.Oneonta sandstone. Loose on the ground at this locality but apparently from this ledge are blocks contain- ing Spirifer mesastrialis Hall, some of which contain large num- bers of specimens; Bellerophon sp. and a scale “ belonging in all. probability to Holoptychius americanus Leidy” according to Dr Eastman were also found. The top of the ledge shows quite a Agriculture of New York. 1846. 1:196. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 163 a heavy dip to the southwest, being at the place measured 2° §, 46° W. This amount of dip seems to show that the coarse, greenish sandstones to the west of north of Jefferson and east of Morseville have been carried considerably below the surface at Jefferson; in fact if the dip be as great to the east of south for the entire distance then the sandstones to the north of Jef- ferson (XXVII A‘) must be some 300 feet below the ledge (XX VII B) to the south of the village. A view of this ledge was given in part 1 of this report on pl. 9. On the Geologic map of New York the base of the Oneonta sandstone is represented consider- ably farther south than the ledge of greenish and red sandstone to the south of Jefferson. SCHOHARIE VALLEY SECTION Crossing the eastern central part of Schoharie county from — the south to the northeast is the Schoharie river,“ which for the greater part of its course from Gilboa to Middleburg has cut a narrow and deep valley lined by steep and often precipitous hills. From Middleburg to the north the valley is generally broader although usually lined by steep hills with rocky slopes. It is a beautiful valley and the view from nearly all of the high hills: io the east or west of the river is inspiring. In the writer’s - opinion the valley is one of the most beautiful in the state. The course of the Schoharie river has been well described by Prof. Guyot who said, “The main Schoharie creek originates at the foot of the Schoharie peaks [in the central chain of the Catskill mountains|, near the head of the Plaaterkill clove, from which it is hardly separated by a slight swell in the swampy. valley bottom.” After describing its course through the Catskills he continues, “ at the confluence of the Manorkill, it enters the mass of the northwestern plateaus, cutting from Gilboa 1033 feet, to Middleburg 640 feet, a deep and narrow valley, the bottom of which is from 1000 to 1800 feet below the general level of the aOn most of the maps this stream is uted. Stuotiarie. preeke pub ou uo eee ne length, over 76 miles, its volume of water, and the large area of country drained by it and its tributaries, the writer prefers to call it a river. 164 . NEW YORK STATE MUSEUM country it traverses, while the occasional flat bottoms in it at e : 7 Blenheim, Breakabeen, Fultonham and Middleburg, rarely attain more than half a mile in width. Its course from Blenheim, : through Middleburg, Schoharie and Central Bridge, -where | it receives the Cobleskill, is alternately to north-northeast and north. From this place instead of following the broad valley through which runs the Albany and Susquehanna railroad ~ {now Susquehanna division of the Delaware and Hudson R. R.], — it leaves it and cutting its way at right angles through the high : hills which border the Mohawk, it finally enters that river near Fort Hunter, after a course of over 76 miles. The contrast of the broad, open valleys between the moun- | tain chains above described [the Catskills], and the narrow and deep cut of the Schoharie creek when passing thous the piateau region is a feature to be noted. _ This drainage which sends the waters of the Catskills all the way around to the Mohawk to come back by the Hudson, after ‘ a course of 175 miles, to within 10 miles of their starting point — is certainly remarkable, and betokens a very peculiar physical structure. This is made more striking by the fact that on both sides of these highlands the waters of the valleys of the Cats- kill and Esopus creek flow, as we might have expected, from the western plateaus directly to the Hudson river. These three streams, which are so near each other, flow in opposite direc- tions, and it seems as if this plateau of the Catskills had been lifted up on its eastern part to a higher level from which its waters were sent in the opposite direction.” — The importance of the Schoharie valley for geological investi- gation was early recognized by geologists and Mather wrote as follows concerning that portion of the valley about to be de- scribed more particularly, “The valley of Schoharie creek be- tween Middleburg bridge and Gilboa, also offers fine oppor- tunities for examining these strata [of his Erie division] and the valleys of the small streams that flow into the Schoharie kill — aAmer, jour. science, 3d ser., 1880, 19: 442-45, wet = ef ERT, i= 320 7E Seu: CR, 1m ie Me iy . : 5 A GEOLOGY LAL SECTION eters SCHOMML RIVER 8 SCHOHAHIE 10 CULBUA § = MILL VALLEY VROMAN'S Nase “FULTONHAM / fife LEVEL OF MIDOLEBURE CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 165 offer still better opportunities.’”” While a section “from Esper- ance in Schoharie co. up the valley of Schoharie creek to Deep * Clove” gives a good idea of the steep hills and narrow valleys, and fairly accurate limits for the lower formations. The limits and correlations of the later formations not being clearly under- stood at that time are not represented with the same degree of accuracy. ; Emmons referred frequently to the Schoharie valley region and in describing this route to the Catskills said, “ The whole New York system is traversed by this route, and it leads up a beautiful valley, on the sides of which the strata are finely exposed in receding terraces or steep escarpments. Beautiful ‘cascades and splendid scenery gratify the sight at every turn; while to the geologist the succession and stratigraphical arrange- ment is so clear and satisfactory, that all doubts are dispelled. ‘The advantages of this route are decisive, in consequence of the fine field at Schoharie, where the succession is over a complete division of the Helderberg rocks; the Erie division is full and complete also, and may be observed first in the rounded hills about Schoharie village, dipping in the direction of the route of the creek; and the succeeding members slowly follow each other, till, finally, at Gilboa, the Catskill rocks are found at the base of the high ranges which have hedged in the creek for 25 miles.’’¢ The rocks along the Schoharie river from Gilboa to Middle- burg were also measured by Andrew and Clark Sherwood in 1873 under the direction of Prof. Hall and the section was published in 1878.4 On the accompanying “ Geological section along the Schoharie river from Schoharie to Gilboa” the attempt is made to indicate something of the topography of the western side of the valley and the most conspicuous outcrops of rocks. There is no topo- eraphical map of that portion of New York and so on account - of the absence of sufficient data it was only possible to indicate © the most general features of the topography. a Geology of New York. 1843. Pt 1, p. 321. b Ibid., plate 25, fig. 5. e Agriculture of New York. 1846. 1:197. d Proc. Amer. philosophical society, 17 : 347-49. 166 NEW YORK STATE MUSEUM Middleburg Biadelohire is the next township in the Schoharie valtey south of Schoharie, a famous geological region on account of the excel: | lent outcrops of the Helderberg and Corniferous series on ee high hills to the west and east of Schoharie village, known as fe West and East mountains. On the accompanying geologic section ne of the Schoharie river, a section of West mountain 690 feet in és thickness is given showing the formations from the upper part | 7 of the Hudson river into the Onondaga limestone. The section ie will not be described more fully in this report since it is outside of the formations under consideration. The central part of Middleburg township is crossed by the ix Schoharie river and the northern end of its gorge may be re- garded as terminating near the southern border of the town- ship. The geological formations underlying the greater part of the township are the Marcellus and Hamilton; the northern part ~ of the township is cut down into the rocks of the Corniferous, © Oriskany and Helderberg series, and to the south of Middleburg i : village near the top of Moheganter hill in the southern part of — the township rocks of the Sherburne formation occur. The top. of the Onondaga limestone shows in the Schoharie river about one half mile below Middleburg village where it makes a small fall;¢ and by the Middleburg and East Cobleskill highway cross- ing of the brook in the northwestern part of the township, some — 190 feet above the river level. This gives a dip of over 105 feet a mile for the limestone. To the east of Middleburg village is a prominent hill, the upper part of its western face being nearly perpendicular and the locality _ is known as “ the cliffs.’ The rocks are sandstones and arenace shales containing Hamilton fossils which belong in the lower part of the formation. The view of this cliff given was taken from the eastern part of the village. XXXVII B2. On the eastern side of the river one mile south of Middleburg and about east of the prominent hill on the western side of the river known as Vroman’s Nose, are ledges of sandstone and shales along the lower slope of the northern part of Mohe- ganter hill. The base of these rocks is approximately 160 feet a Proc. Amer. philosophical society, 17 : 349. y x Tey we, ae 85! 1480" |--——— we Grayish and pica sandstone rr * deta 5? ce 65’ : Pi Jac tS \ > i 1365’ — ——| D® Red and ereen mottled sandstone a shale + : : 41335’ ———| D® Green shales 145’ Sherburne =< . ; ee eee) aan blue sandstone : ae 340’ | D® Covered tt / a Sa" 20’ | D? Quarry of blue sandstone and shale ek) Bee Hamilton se 515’ | D* Mainly covered 315’|—_—-—__, Bridge across creek 24 miles S. E. of Midalebong 315’ | D* Covered 0’ |———|! Schoharie river at Middleburg CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 171 | Fulton — The next township to the south in the Schoharie valley is Fulton which lies to the southwest of Middleburg and east of Summit. Its eastern-central part is crossed by the Schoharie river bordered by steep and high hills that south of Fultonham on the western side and north of Breakabeen on the eastern side have nearly perpendicular cliffs several hundred feet in hight. The western line of hills is broken by the creek at Fultonham and again by Panther or Kenhuragara creek between Fultonham and Breakabeen, and the eastern line by Keyser’s creek and a brook at Breakabeen. XXXVII C. In the southern part of Middleburg to the east of the Schoharie river is Moheganter hill which extends into Fulton township. Three miles southwest of Middleburg village, near “the schoolhouse of district no. 11, the face of the hill is cut by a small brook and at this locality a road leaves the river road and climbs to the top of the high hill. A section was measured from the level of the Schoharie river along the brook and highway to the top of the hill at this locality which from a geological stand- - point is a very interesting study. The section is near the Middle- burg-Fulton township line being partly in each township, and its | base is about opposite Watsonville on the western side of the river. The lower 200 feet are covered, largely by sand; but then a ledge of coarse, arenaceous shales and thin sandstones (C?) is reached. This ledge is in the woods where it forms a cliff 30 feet high. The dip is between 13° and 2° 8S, 70° W. The rocks contain abundant Hamilton fossils and belong near the middle part of the formation: The following fauna was obtained: 1 Spirifer mucronatus (Con.) Bill. (c) 28. granulosus (Con.) H. & C. (rr) 3 Athyris spiriferoides (Eaton) Hall r (c) 4 Camarotoechia congregata (Con.) H. & C. (r) 5 Microdon (Cypricardella) tenuistriatus Hall (?) (rr) Imperfect and worn. _ 6 Chonetes mucronata Hall (c) Specimens larger than the figures of this species. 5 glee | NEW YORK STATE MUSEUM | 7 Chonetes deflecta Hall 5 reo eta 8 Palaeoneilo tenuistriata Hall he . | (Tae hah ict 9 Macrodon hamiltoniae Hall eS 10 Grammysia bisulcata (Con.) Hall ie is ae 11 Tellinopsis subemarginata (Con.) Hall (rr) 12 Pterinea flabella (Con.) Hall Soe (EEE: 13. Cyrtolites (Cyrtonella) pileolus Hall (rr) From the top of this ledge for 135 feet to the schoolhouse at the road corners there are occasional outcrops of arenaceous - shales, and then for 305 feet along the road and brook the rocks . are mostly covered. By the side of the highway just above the — house of Mr George P. Bouck and about one mile above the river . road is an outcrop of from eight to 10 feet of Hamilton shales (C4). Those at the base are rather fine but the upper ones are coarser. The shales are mainly argillaceous and contain numer- ous Hamilton fossils. The list is: 1 Spirifer mucronatus (Con.) Bill. - ; (ry 2 Cryptonella (Euneila) incklaent Hall | (c) 3 Athyris spiriferoides (Eaton) Hall (rr) 4 Productella dumosa Hall (?) | Bercy) 5 Camarotoechia prolifica (Hall) H.& ©. (rr) 6 Gomophora hamiltonensis (Hall) Miller (rr) 7 Nuculites oblongatus Con. ' (Br) 8 Palaeoneilo constricta (Con.) Hall | , (rr) 9 Cumtaria elongata (Con.) Hall (?) (rr) rt Imperfect. 10 Actinopteria boyd (Con.) Hall ey a 75 feet higher and 755 feet above the Schoharie river are very, thin, bluish, argillaceous shales (C°). In a layer of somewhat coarser shales is an abundance of specimens of Nyassa arguta Hall; while a little higher are some thin layers of concretionary ~ sandstone. These shales are referred to the Hamilton formation and the following fossils were collected: 1 Cryptonella (Eunella) lincklaem Hall (c) 2 Athyris spiriferoides (Eaton) Hall (a) Abundant in a layer of thin, shaly rock. Mo. 37,0. SECT / ON WEG MUL 3 Mt.S.0F MID0LEBUPEH. 350 Sos GRAY SHALY SANOSTONE IN 2040. Exo FEO SHALE TOP OF HWlit /W FIELO, 330 95) PARTLY COVERED. CETBES, rs C® | Red sAnwosroweE ONEONTA. PARTLY COVERED, ConRse GRAY SANOSTOWE. FEW ourcfoes, 6reenisu sHALES .SHEFBUAWVE. MosTLy CovERED. Nyassa Ano orwen HAMILTON Fossics. 75"\ CovERed. SHALES wiTH HAMILTON FOSSILS MosTLy COVERED ALONE FOAD AND BROOK. SCH 00L-HOUSE AT CORNERS MosTrv COVERED; SOME EXPOSURES OF THIN SANOSTONES, AHENACEOUS SHALES 7O THIN SANOSTONES. CovE RE 0, PARTLY BY SAND, LEVEL OF SCHOHARIE RIVER OP WATSOWV/LL En CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES Se 3 Camarotoechia prolifica (Hall) H. & C. ~ (a) Abundant in same layer as above. 4 Spirifer mucronatus (Con.) Bill. (rr) 5 Nyassa arguta Hall (aa) - 6 Paracyclas lirata (Con.) Hall ) (rr) 7 Goniophora hamiltonensis (Hall) Miller (rr) 8 Pterinea flabella (Con.) Hall (rr) 9 Liopteria bigsbyi Hall (rr) | 10 Cyrtolites (Cyrtonella) mitella Hall (rr) By the roadside 240 feet higher and 995 feet above the Scho- harie river are thin, greenish, argillaceous shales and some that are arenaceous (C’). These shales are referred to the Sherburne formation which they closely resemble in lithologic appearance. For the succeeding 125 feet the rocks are well covered though there is an occasional outcrop of the greenish shales; then a coarse grained, greenish gray sandstone (C8) with crossbedding is reached. Then the slope for 115 feet is partly covered with an occasional outcrop of the grayish to greenish sandstone. 55 feet above the lowest ledge of these sandstones are thinner gray sandstones, and in some rather shaly layers a few imperfectly preserved fossils were found—a remnant of the Ithaca fauna— which at that locality, by the changed conditions of deposition, _ had narrowly escaped complete extermination. At 1235 feet above the river level is a thick, unusually hard ledge of reddish, indurated sandstone. Above, the slope though partly covered shows frequent outcrops of red and greenish shales. 95 feet above the top of the reddish sandstone at the top of the brow of the hill are soft, argillaceous red shales. On the highway about 20 feet higher are grayish, shaly sandstones (C"), and 50 feet higher is another outcrop of coarse grained, greenish gray sand- stone. The bedding is somewhat irregular but not thick and _ there is a layer of breccia. The only fossils found in place in these upper deposits were fragments of plant stems. By the side of the road, in loose pieces above the red shales, specimens of Tropidoleptus carinatus (Con.) Hall, Spirifer mucronatus (Con.) Bill. and Camarotoechia prolifica (Hall) H. & C. were found. It is ’ not probable, however, that these frasments came from tee part ~ veo Ph ate Er ky KreE ae ne es i mt cn 3 ras sy 174 NEW YORK STATE MUSEUM x ein aD of the hill, but they were undoubtedly left by the ice sheet near a the summit of Moheganter hill. On a stone wall in this vicinity = “a large flat blocks of sandstone were seen which contained the fol- Be lowing species, the first one occurring in large numbers: we. e 1 Chonetes coronata (Con.) Hall (aa) a : 2 Tropidoleptus carinatus (Con.) Hall (a) ; os 3 Camarotoechia prolifica Hall Sete (c) ae 4 Spirifer mucronatus (Con.) Bill. (r) ei 5 Athyris spiriferoides (Eaton) Hall ft aaa “(eis From this last outcrop to the top of the hill at the corners, men- — ae tioned in section XX XVII D, is 40 feet which makes it 1440 feet ae above the level of the Schoharie river at its base. The baromet- e = ric section from Middleburg village up the Little Schoharie and the eastern slope of Moheganter hill (XX XVII D) to the road cor- : me ners made it 1500 feet; so in the elevations there is probably nota very serious error in the case of either section. This section is by Wry + eee? here represented diagrammatically. On account of the covered sei slope it is not possible to indicate closely the line of division be- — wae! Sy ees tween the Hamilton and Sherburne formations. There are at f least 755 feet of rocks above the level of the Schoharie river be- longing in the Hamilton and probably part of the succeeding — i i covered 240 feet belongs in the same formation. The 240 feet above the covered zone to the base of the heavy red sandstone is ao referred to the Sherburne and Ithaca formations, the thickness of = which probably should be increased by a portion of the under- : lying covered zone. The rocks from the base of the red sand- stone (0°) to the summit of the hill are referred to the Oneonta formation. It is clearly recognized that to the west of the Scho- pe harie river, rocks at this horizon are not red and are not called Oneonta but are referred to the Ithaca formation. A little . farther east, however, along the Schoharie-Albany co. line and to the eastward, the red rocks near this horizon and still lower have been mapped and correlated with the Oneonta forma- tion. In that region it is impossible to follow any line of di- vision between the Ithaca and Oneonta formations, for. the <7 CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 175 Oneonta has replaced the Ithaca in the same manner as the Cat- kill replaces the Chemung in Delaware co., and the author considers it advisable to follow the precedent of the state sur- vey and so apply the term Oneonta formation to these rocks al- though it is quite true that they are synchronous with rocks. which in the Susquehanna valley are referred to the Oneonta, Ithaca and upper Sherburne formations. The above statement | explains why the Oneonta formation is represented on the Geologic map of New York so much farther north on the eastern than on the western side of the Schoharie river; and correctly so, provided the lower mass of coarse greenish gray and red sand- stones with red shale, which can not be separated from the Oneonta formation in its typical region, be referred to that forma- tion. On the eastern side of the Schoharie river the author has _ referred the rocks to the Oneonta formation beginning with the lowest red sandstones or shales of any considerable thickness. The sandstones below are frequently coarse and similar to those in the Oneonta, but the stratigraphic position and the occurrence of a few fossils in the alternating shales have decided the author to correlate them in general with the Sherburne formation. On the Geologic map of New York the top of Moheganter hill and the high land between Breakabeen and Franklinton are represented as in the Hamilton formation (the upper partof whichincluded the Ithaca and Sherburne formations) but it should be represented in the Oneonta for the rocks of corresponding stratigraphic posi- tion on the high ground to the northeast of Franklinton and to the south and east of Huntersland are so represented. On the accompanying geologic map it will be noticed that the base of the Oneonta’ formation to the east of the Scho- harie river is represented nearer the western brow of the steep hills than on the Geologic map of New York and that it runs north into the northwestern corner of Broome township and then southeasterly along the side of the steep hill to the southwest of the upper part of the Catskill creek, till it crosses that creek be- low Livingstonville near the county line. To the northeast of the Catskill creek across the northeastern part of Broome town- : 176 i NEW YORK STATE MUSEUM ~ ship into Albany co. the lines on the two maps agree quite closely. On the Geologic map of New York published in 1844 all _ the high country in Broome and Conesville townships in the east- ern part of Schoharie co. is mapped as belonging to the Portage and Chemung formations, which were not separated on the map. 5 Along the highway from the corners at the schoolhouse of dis- — trict no. 11 in Middleburg to Houston Corners east of Breakabeen — there are occasional ledges of shales and sandstones which are in the upper part of the Hamilton formation. Opposite Blen- heim hill, the name applied to the high hill on the western side of the river between Fultonham and Panther creek, on the road- _ side are fairly gritty blue, sparingly fossiliferous shales (X XIX B?) from which the following species were collected: Pe ee ee 1 Tropidoleptus cariatus (Con.) Hall / . (Oies2 ee Camarotoechia congregata (Con.) H. & C. Be Ot 3 Liopteria sp. | (rr) Badly broken specimen. 4 Modiomorpha subalata (Con.) Hall (?) (rr). Imperfectly preserved specimen. XXIX A. On the eastern side of the Schoharie below Breaks been there is a perpendicular cliff of shales alternating with sand- stones rising from the river estimated as between 60 and 70 feet. high, then a line of trees, then another perpendicular cliff and at the top a third one. A hill crowns the summit and the entire. exposure is known as Wauhalla mountain. A view of this cliff from near the river road on the western side is here shown. A section was constructed from the river level at the highway bridge below Breakabeen through Houston Corners: to a point near the top of the hill to the north of east of the Corners and the diagrammatic form is here given. On the western bank of the river at the highway bridge below Breakabeen are blue, somewhat irregular shales alternating with blue sandstone layers varying in thickness from two inches to a foot. The shales at the northern end of the bridge contain large numbers of Paracyclas lirata (Con.) Hall associated with other Hamilton N0 29,4. SECTION LAST OF LHEAKAGLLN ANOWAUHALLA MOUNTA TIL, NEAR TOP OF Ale, Coveren. PLENTY OF LOOSE RED SANDSTONE, GREENISH BRECCIA (Cay PE @BLES) Coveréo. THIN BFODEO BLUISH-@RAY SANDSTONE. Covereo. THIN-BE DIED BLUISH-GRAY SANOSTONE, CavER Eo. SANDSTONE. GREEN AR 6/LLACEOUS SHALES, SHERBURNE, Cover En. SANOSTOWE. THIN BLUISH SHALES WTH ABUND= ANT FOSSILS. Cove FE o. THIN-BEDOED 5 ANOSTONE. Cove a Eo. AR ENACEOUS SHALES WITH ABUND- anv HAMILTON FOSS/LS- HousTows CoRWe- ERE. WAUH ALLA fr. HAMILTON. LEVEL OF SCHOHARIE RIVER AT BAIDEE BELOW BREAHABZEEN,. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 177 fossils; while the sandstone layers contain some different species. A layer of ferruginous concretions is noticeable. The dip on the _ western bank is from 1° to 14° S 64° W and on the eastern bank it is more than 1° in amount, west of south (the exact direction and amount were not determined on account of the distance at which the observation was made). ; The rocks next studied (A’) are in a small brook at Houston | Corners, three quarters of a mile east of Breakabeen and 350 feet . above the river. The outcrop consists of coarse, arenaceous shales to shaly sandstones, the latter containing numerous speci- mens of the large Hamilton Lamellibranchs. These rocks are ~ clearly of the Hamilton formation and the following species were collected: 1 Camarotoechia prolifica Hall (r) 2 Chonetes coronata (Con.) Hall (rr) 3 Spirifer mucronatus (Con.) Bill (?) (rr) 4 Tropidoleptus carinatus (Con.) Hall : (rr) 5 Liopteria greeni Hall (rr) 6 Glyptodesma erectum (Con.) Hall (?) (Tey 7 Goniophora hamiltonensis (Hall) Miller (TE)s3 8 Grammysia alveata (Con.) Hall (c) 9 Phacops rana (Green) Hall (rr) 10 Microdon (Cypricardella) bellistriatus Con. : (rr) 11 Crinoid stems On the slope of the hill to the north of east of the ledges in the brook at the Corners, the rocks are covered for 55 feet, when a zone of thin bedded sandstones (A‘*) is reached. This outcrop of somewhat crossbedded sandstones about 10 feet thick is im- — mediately above the road leading northeast from Houston Cor- ners toward the top of Moheganter hill. The dip varies; but — perhaps will average 14° S 20° W. The ledge was not suffi- - ciently broken to enable one to easily determine whether it con- tained fossils or not. About 65 feet above it are thin bluish shales (A*) containing abundant fossils. These shales hardly form a ledge but from the way in which they lie on the surface and are ipadnaes in the Hamilton formation. - gpecies were collected: : 3 | = a] 1 Camarotoechia prolifica (Hall) H. & C. | 2 Ambocoelia wnbonata (Con.) Hall 3 Strophalosia truncata (Hall) Beecher 4 Pterinea flabella (Con.) Hall ' 5 Nyassa arguta Hall . 6 Nuculites oblongatus Con. 7 Palaconeilo constricta (Con.) Hall 8 Nucula dellistriata (Con.) Hall 9 Tellinopsis subemarginata (Con.) Hall 10 Tentaculites bellulus Hall no fossils were found. Then there is a covered slope of 75 feet when, at an altitude of 585 feet (barometric) above the river, the base of decidedly green argillaceous shales (A’*) is reached. “These are capped by thin bedded, grayish sandstones and to- gether they have a thickness of 25 feet. Careful search was Imade in the green shales for fossils, but without success and _. the rocks have the lithologic appearance of the Sherburne to which formation they are referred. After 15 feet of covered aa slope there is a ledge of thin bedded, unfossiliferous bluish gray ; sandstone (A!) about 10 feet in thickness. For the remaining © upper part of the hill the rocks are mostly covered, two feet of a bluish gray thin bedded sandstone outcropping at 685 feet above the river, and a two foot stratum of greenish breccia with — clay pebbles at 745 feet. The hill was examined 70 feet higher to $15 feet, which is near its top, but no further ledges were noticed. On this upper slope of the hill, however, are plenty of loose blocks ~ of red sandstone probably in place near that horizon or perhaps ~ that once capped the hill and through erosion have dropped down ~ : its side. In the above section the Hamilton extends fully 480 Sa feet above the level of the Schoharie river, and a little more CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG-SERIES 179 than 100 feet above it green shales and sandstones are reached ~ which are apparently in the Sherburne formation. | On the _ Moheganter hill section 240 feet higher than the bottom of sim- ilar ereenish shales, also referred to the Sherburne formation is_ the base of the zone of red sandstone and red and green shale fully, 100 feet in thickness. The same thickness above the green shales | on the Houston Corners hill will carry the section slightly higher than the hill was studied. The large amount of loose angular blocks of red sandstone, however, seen on the covered slope of ‘the upper 70 feet of the section indicates the presence of the red rocks on that hill somewhere near that horizon. The Sher- | wood brothers gave a measured section of the Wauhalla moun- tain in their Schoharie river section, the base being the “ gray - shaly sandstone” of their no. 18, while the top is in no. 31 a ““oray sandstone.”* Their section makes the top of Wauhalla mountain between 533 and 605 feet above the level of the Scho- harie river and near the same horizon as the greenish shales on the Houston hill which we have referred to the Sherburne forma- tion. ; ey XXIX X. The highway was followed up Keyser’s creek from Houston Corners nearly to the southeastern corner of Fulton - township; but without satisfactory results on account of the mantle of drift which conceals most of the rocks. On the creek banks some 110 feet above zone A? at Houston Corners are bluish shales and sandstones (X*‘) which are probably in the Hamilton formation although no fossils were seen. From the creek to the highway, approximately 185 feet, the rocks are completely concealed; but on the hill northeast of the road there are two ledges of coarse greenish gray sandstone, one at 420 feet above the creek and the other near the top of the hill at 780 feet above the creek. Loose on the hillside between the two outcrops of the greenish sandstone are numerous large blocks of the red sandstone which evidently occurs somewhere in that part of the ~ hill. The stratigraphic position of these red sandstone blocks agrees in a general way with its supposed horizon near the top a@ Proc. Amer. philosophical soc. 1878, 17 : 348. of the hill east of Houston iets This section 1 is the following diagram. ae . an 3 aay X MUX _ 420’ |———| Greenish sandstone SECTION | OF HILL NORTHEAST OF KEYSER’S CREEK oe 780’. |-—-—| Coarse greenish sandstone near top of hill fee - 360’ | Large nu mbers of loose blocks of red sandstone 420° | 1851 Highway. X? covered X* Blue shales and sandstones ? (pope Keyser’s creek, 110 feet above Houston Corners XXIX M. Aboye Keyser’s creek, a smaller stream than it enter the Schoharie river at Breakabeen. A section was yer ton fossils and the following oe were collected: 1 Camarotoechia prolifica Hall 2 Spirifer mucronatus (Con.) Bill. 3 Nucula bellistriata (Con.) Hall 4 Grammysia arcuata (Con.) Hall 5 Homalonotus dekayi (Green) Emm. 6 Tentaculites bellulus Hall (?) next outcrop, consisting of coarse grained grayish sandeteae ary, fe é ie ae which split into thin layers is 540 feet above M?. -The only ? : fossils seen were fragments of plant stems and the outcrop 1s well toward the head of the small valley. 100 feet higher, how-— 33 CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 181 ever, or 840 feet above the Schoharie river and probably across - the township line in Gilboa, perhaps three miles.from Breaka- | been, are fossiliferous rocks (M°). At the base of the outcrop is | just a little greenish, argillaceous shale, while above are bluish gray, thin sandstones and shales containing some fossils. Speci- mens of Tropidoleptus carinatus (Con.) Hall are common, and Spirifer mucronatus (Con.) Bill. occurs less frequently. Above this fossiliferous zone there is another long drift covered slope, but 410 feet higher, near the turn toward North Blenheim, red argillaceous shales outcrop on the highway. This section may | be tabulated as follows: SECTION OF HILL EAST OF SOUTH OF BREAKABEEN INTO NORTHERN GILBOA XXIX M 4250’ |_——| M® Red shale near turn to N. Blenheim - Oneonta 410’ | M* Covered | 340’ |——-—_| M® Bluish-gray shaly sandstone with fossils 100’ | M® Covered 740’ |——— M* Ooarse grained grayish sandstone Sherburne 540’ | M® Covered 200’ |\—_——; M? Bluish fossiliferous shales. Hamilton 200’ | M+? Covered 0’ |\_——_| Schoharie river at Breakabeen . AS so much of this iit is covered 2 is difficult to correla a different zonts with those of the sections at Houston Ce and ee hill. here was no So of the red Bee section as in Moliceantor hill and there is a peace: thickness a the Ithaca formation. - 3 ‘(XXXVI A. ee. to the western side of the Scholiame ae collected: 1 Chonetes mucronata Hall (?) 2 Styliola fissurella Hall - In certain layers. | 3 Orthoceras subulatum Hall (?) Fragment. 4 Crinoid segment The Sherwood brothers in their Schoharie section give above | the Onondaga limestone 25 feet of black slate and shale (dence 3-5),” without correlating it with the Marcellus; but they aie ported that above these lower black shales 305 feet were covered ‘3 which would more than include the entire Marcellus formation. — a Proc. Amer. philosophical soc. 17: 349, IN EMG (SIV OTOL WEST OF FULT ONTAM ALONG FOAD TOWARD VY FULTON, 955 SS GRAYISH SANDSTONE AT TOP OF HILL LAST FOSS/LS SEEW! SHALES witH HAMILTON FOSSILS BLUISH SHALES HAAMILTON, THIN BLUISH SANDSTONE. 2LOV 260 - = = = BLUISH SHALES WITH ae faracyclas 80 2 Re. SCHOHABPIE RIVER. No. £8, XN. SECTION OF HILL SOUTH OF HUNTER CELA Sum nair. COARSE-G6GRAINED 6REENICH-CRAY SANDSTONE GLUISH SHALES WITH ABUNDANT FOSSILS. /THACA GREENISH SANOSTONE SHE RE URNE GREENISH SANDSTONE GLVISH SHALES, THREE CORNERS TWO MILES BEL0w WesrFuLTon. + 25 | SHALES AND SAN OSTONES K* | Ow PauTHER CHEER. Ras| FARTLY COVEFED HAMILTON fe. LEVEL OF SCHOHARIE RIVER AT- ~| /#0N BRIDGE BELOW BREAHABEENW. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 183 In loose blocks in the Mill creek valley probably carried down by the creek, the following Hamilton species were collected: 1 Spirifer mucronatus (Con.) Bill. — (a) - Specimens of the very mucronate type. 2 Chonetes coronata (Con.) Hall : (rr) 3 Camarotoechia congregata (Con.) H. & C. | (ce) To the southwest of Mill creek is Vroman’s Nose which rises some 600 feet above the level of the Schoharie river. The lower part of the southern face has a steep slope largely covered by debris from the upper part of the hill, while the upper portion is a perpendicular cliff composed mainly of coarse, arenaceous ~ shales and sandstones. . It is certainly a commanding hill when seen from its foot or at Middleburg, and when seen from the much higher hills to the southwest it looks like a hill blocking the Schoharie valley. A picture of this hill which, unfortunately, like photographs since taken does not give a very distinct im-_ pression appears in Emmons’ Agriculture of New York.” The hill was studied in a rather hurried manner but, approximately 250 feet above the river is the base of the rocks which continue for 3¢Q feet to the top of the hill, (A*). The lower rocks are dark — gray shales above which toward the top of the hill are rather blocky shales and thin sandstones. Hamilton fossils occur in the shales in moderate abundance while in some of the coarse, | shaly-sandstones there are numerous specimens of Spirophyton and Spirifer granulosus (Con.) H. & C. These rocks all belong in the lower part of the Hamilton formation and according to - the Sherwood measured section there are 372 feet exposed in the hill, below which are about 200 feet covered.o On the bare : sandstone ledge at the summit of the hill are conspicuous glacial striae, some of them quite deep, which run W 10° S. The following is an approximate section of Vroman’s Nose. avy. 1, plate 6, , 6 Proc. Amer, philosophical society. 17:348 are pos ae ee ele FAST en bamn| pare verve Illi area cn mete ee ale. SECTION OF VROMAN’S NOSE — KXXVIT A’: 610’ |——— Top of hill ae -Arenaceous shales and sandstones Hanulton x eee 0S eres A? Approximate position shale on Mill creek west of Fultonham, was soleehel hastily studied. This a Ses which is here given is about opposite the one of Moheganter- oes hill on the eastern side of the river. Along the road for some 8 280 feet outcrops are very rare, then blue shales occur contain. a ing specimens of Chonetes coronata (Con.) Hall, Paracyclas lirata _— aa (Con.) Hall and other fossils. From this zone to the summit of i the hill the rocks consist of a succession of blue argillaceous’ shales alternating with sandstones, all of which are apparently in the Hamilton. The highest fossils collected were at 760 feet — above the river level and for the succeeding 195 feet the rocks are mostly covered till the summit of the highway is reached. ee where there is a ledge of bluish gray sandstone. Above the road a ‘ ‘ 2 * sa “ , Le oe r . a »” te 4 is F - a ae Ae oe ts Py. Sa eae Somes eee TS a ma = SHIVHS NOLTINVH ONIG ‘WVHNOLTIOW 40 HiOOs ,,‘HLIVd MOL, tO GNH HIYON : 4 s ied ane” CoP eign 4S OR i. wes \ 8 %4Bld NE, Ny Dts 4s Ae CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 185 ‘on the northern side there is a ledge of thin, crossbedded, grayish sandstone. From the river to the road summit is, according to _ the barometer, 955 feet, which as already stated is apparently all Hamilton. If this correlation and Sherwood’s statement that the “top of Vroman’s Nose, passes under water at lower end of tow-path road [which is just south of Fultonham] ’’” be correct, then the Marcellus and Hamilton formations on the Schoharie river have a thickness of at least 1670 feet, which, as will be shown later is probably an underestimate rather than an over- _ estimate of their thickness. To the south of the summit of the read, Blenheim hill is considerably higher, perhaps 200 feet, but the writer did not have the opportunity to examine it. The eastern side of Blenheim hill is very steep and rocky and along the tow-path road are cliffs of argillaceous shales and sandstones. “The rocks along the highway belong stratigraphically in the lower part of the section from Fultonham west across the aiorthern end of the hill. ‘XXVIII X. This section is along Panther creek from the Schoharie river to about two miles below West Fulton and then up the hill to the southwest of the creek. For about 90 feet along the lower part of Panther creek the rocks are mostly covered when the foot of the gorge at Bouck’s falls is reached. This narrow glen is lined by clifis of coarse shales and thin sandstones {X*) which are apparently over 100 feet in hight. Picture rock, on the southern bank a little below the falls is some 85 feet above the creek level at its base; while from the creek level below the falls to the top of the shales under the hotel is approximately 130 feet, or some 220 feet above the Schoharie river level. The — gorge iS narrow indicating its recent formation and has been cut from rocks of Hamilton age. Some distance farther up the ereek and perhaps not much higher than the top of the shales in the cliff at Bouck’s falls is the upper end of the gorge. The rocks (X*) consist of shales and sandstones, some of the latter being quite massive. On the northern side of the creek the ex- posure is some 25 to 30 feet in hight and is labeled the Blarney a Proc. Amer. philosophical soc. 17:348. 186 ' NEW YORK STATE MUSEUM stone. The dip is ee: heavy, being about 4° 8 30°. We Some of the shales contain. numerous specimens of Spirifer os granulosus Con. and other Hamilton fossils. On the under side’ Bees of a sandstone stratum just above the creek are large numbers of 2 : the very mucronate form of Spirifer mucronatus (Con.) Bill. as- ia sociated with Chonetes coronata Con. The fossils and the strati- a graphic position of the zone show that it is in the Hamiltonforma- - rf ee tion. The species listed below were collected at this locality: 3 oo 1 Spirifer granulosus Con. ‘i fa : : cS : 2:8. mucronatus (Con.) Bill. - . ohh eee 3 Tropidoleptus carinatus (Con.) Hall (rr) = ag 4 Camarotoechia prolifica (Hall) H. & C. . (¢) ‘ : 2 = 5 Nyassa arguta Hall | st ae = 6 Orthonota undulata Con. | | (rr) 7 Chonetes coronata (Con.) Hall re) ats a Above the rocky gorge just described, well toward West Ful- - ton, Panther creek fiows in a deep gorge, but the sides are covered _ with drift, clay and boulders of all sizes so that the bed rocks are He = concealed. At the three corners, perhaps one and one half miles | below West Fulton, the section leaves the valley of Panther creek and follows the highway turning westerly which ascends 3 ee the steep hill that rises to the south of the creek valley. The a road corners, by the barometer, are some 190 feet higher than the — glen at X2 and the slope of the hill for over 800 feet is pretty gen- ee erally covered by drift. There are a few exposures along the a highway in this 800 feet of elevation, as, for example, X4, 145 feet se above the corners where fine, bluish, argillaceous shales and —-_— Somewhat greenish sandstones occur. Again, 550 feet higher, . toward the top of the hill and west of the first road turning to — the south, is a ledge of rather coarse grained somewhat greenish gray sandstone (X°) which has been referred to the Sherburne | formation. About 145 feet higher, or by the barometer some 1280 feet above the level of the Schoharie river at the bridge be- z low Breakabeen, are the bluish, argillaceous shales of X®. This 7 locality is well toward the summit of this part of the plateauan@ is to the west of the second road turning to the south. It is am a NOLTINVH ‘STIVHA S,sMOMog / 00 0NOd NYO HOSKIN Ys ix 6 941d CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 187 important outcrop, for some of the thin layers of the bluish shales contain abundant specimens of a few species of fossils. Spirifer : mesastrialis Hall is a common species and this zone is in the Ithaca formation which covers the high part of the plateau to the © south of Panther creek and west of the Schoharie river in the southern part of Fulton township. In coarser shales above the bluish ones the fossils are not so common. The following species. were collected in a few minutes and a thorough search would undoubtedly materially increase the number: 1 Spirifer mucronatus (Con.) Bill. (a) 2 8. mesastrialis Hall (c) 3 Orihonota undulata Con. - (c) 4 Sphenotus truncatus (Con.) Hall (a) | 5 Schizodus appressus (Con.) Hall (rr) : 8 6 SN. ef. elipticus Hall - (r) y Grammysia (Sphenomya) cuneata Hall (?) (r) Specimens broken and imperfectly preserved. 8 Palaeoneilo cf. plana Hall (rr) 9 Liopteria bigsbyi Hall (r): 10 Athyris spiriferoides (Eaton) Hall ape oS 11 Orbiculoidea cf. media (Hall) H. & C. (PE The pedicle passage seems to be wider than in the figures of this species and scarcely connected at margin. About 45 feet higher, lacking but 10 feet of the summit on the highway or approximately 1335 feet above the level of the Scho- harie river, is a coarse grained somewhat greenish gray sandstone (X‘). On the next ridge to the west, atthe same level as X’, is another outcrop of the coarse grained, massive sandstone on which glacial striae are well preserved, their direction being from then e toward thes w. : XXVIII Y. Nearly one and one half miles west of West Fulton is a road which turning to the south climbs the steep hill on the southern side of Panther creek. A section was followed along this ~ highway which is about two miles west of XXVIII X and partly parallel toit. The highway bridge across Panther creek near the base of the steep hill is approximately 280 feet above the level of * 188 _ NEW YORK STATE MUSEUM the creek in West Fulton. The rocks wherever exposed along Se the lower slopes of the hills bordering this part of the course of Panther creek are clearly of Hamilton age. On the highway 375 feet above the bridge, or 655 feet above West Fulton are coarse, — irregular, bluish shales, (Y*) which contain plenty of fossils. The species so far as noted in a hasty examination are Hamilton and ~ this zone is considered to be near the top of the Hamilton forma- tion. About 85 feet higher, or approximately 1190 feet above the Schoharie river, is a prominent outcrop of massive, greenish gray to bluish sandstone (Y®) on the highway leading south well — | toward the corners. The sandstone is quite coarse grained, some 15 feet being exposed, and one layer shows ripple marks. This — zone is referred to the Sherburne formation, and it will be re- called that a similar sandstone in the section to the east (X®) 1135 feet above the Schoharie river was also considered as in this formation. Some 195 feet higher on the main east and west road on top of the plateau is a ledge of thin bedded sandstones {Y"). This ledge crosses the highway just west of schoolhouse no. 6, in a straight line about two and one half miles southwest of West Fulton, approximately 950 feet higher and is at about the -summit of this part of the plateau. The sandstones are moderately fossiliferous, Spirifer mesastrialis Hall (?) being the most common species. The rocks belong in the Ithaca formation, which, as stated in the description of section X covers the high part of the plateau to the south of Panther creek. The follow- ing species were collected: 1 Spirifer mesastrialis Hall (?) ie (¢c) Too imperfectly preserved to show whether there are fine Striae or not. 2 Palaeoneilo emarginata (Con.) Hall var. (r) The form with only a faint posterior constriction. | 3 Bellerophon patulus Hall gb) Pee 4 B. acutilira Hall (2) "(pepe 5 Cyrtolites (Cyrtonella) pileolus Hall (?) (rr) | Imperfectly preserved. 6 Pectinidae sp. (rr) Too imperfect for generic identifieation. phe each 15 740 ma SCF Noa£8,V. SECTION OF H/LL SouTrH OF LYNTHLE ALLA SOUTH-WEST OF UW FULTON. Ro SSS. y7 | Summuir of wee THIN-BEDOEOD SANDSTONE WITH Some FOSSILS ITHACA SHALES WITH FOSSILS OW SOUTH SIDE OF fyLL, /THACA HEAVY BLUISH~ GRAY COARSE- CRAINED SANDSTOWME,. SHERBURNE 6S | Coveren YE ¥2 CosASE HAMILTON GHALES WITH PLENTY oF FOSSILS 375| LOweR paar OF HILL y2 | SeurH OF AsntHeR CREEH, BRIDGE ACROSS PANTHER CREE APQVE WEST FurTroy, g00} HAMILTON esrrey covEREO No.6, V. SEC¢T/ ON ON WESTERN SIDE OF SUHIHIME LVL} Berween BRtAMA BEEN AN BLEN HEM. [55,5 Pe GRAVY SANOSTONE OW ROAD AT SUM /T =a OF REbION. ay COARSE ORAVISH SANDSTONE LOOSE ¢ (4 CARCE AMON. LAAGELY COVERED ee ITHACA Zz THIN GEOIQDED GRAVISA FTO GLVYISH-ERAY CAMODSTOME . MAINLY COVERED. HEACY SANDSTONE 1 RORQ. Resa Cove Reo. (80 (Se Sd 5 | Seis wnewaceous suates wire rossite. HAMILTON BLvisH SHALES LEVEL OF SCHOWABRIE RIVER - ‘ i a j 1 SAS cs o ay hhh Pre i r % = sh Qi G ‘ > oie, oe BRENT i Gi ¥ ets CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 189 XXVIII W?. Perhaps one half mile farther west and some 170 feet lower along the banks of a brook to the south of the road isa good exposure of bluish, argillaceous shales. Stratigraphically these shales belong in the lower part of the covered interval of Y® and being in the Ithaca formation indicate that the greater part of the zone Y® belongs in that formation. The species found | at this locality are the following: 1 Spirifer mucronatus (Con.) Bill. (ce). Some of the specimens are very wide and mucronate. 2 Spirifer mesastrialis Hall | (rr) oN. fimbriatus (Con.) Bill. | (rr) 4 Ambocoelia umbonata (Con.) Hall (?) (rr) Imperfectly preserved. “5 Sphenotus truncatus (Con.) Hall ae Cec): 6 Paracyclas tenuis Hall | (rr): 7% Liopteria dekayi Hall ; (rr). 8 Gomophora sp. (rr) Only posterior part of specimen preserved. 9 Tentaculites sp. (rr) 10 Grammysia subarcuata Hall , (rr) 1+ Crinoid segments In the above section, if the top of the Hamilton formation has been correctly located at Y° then it gives information upon which. an estimate of the thickness of the Marcellus and Hamilton for- mations may be made. The barometer made West Fulton about 450 feet above the Schoharie river level, while in Sherwood’s section the thickness of the rocks from the top of the Helderberg limestone to the base of Wauhalla mountain, which is about oppo- site the mouth of Panther creek, is given as 920 feet”. This gives 920+450+655—2025 feet minus the amount of dip from the mouth of Panther creek to the bridge across the creek west of West Ful- ton for the thickness of the Marcellus and Hamilton formations. If in section XXIX A east of Breakabeen and Wauhalla mountain: the zone A®, 585 feet above the Schoharie river, marks the top of the Hamilton then it is approximately 485 feet lower than in the section XXVIII Y and since the distance between the two locali- a@ Proc. Amer. philosophical soc., 1878, 17 : 348-49. ately 80 feet a mile. The istanee from the cnanee see Pau creek to the bridge west of West Fulton is four and one four ‘miles and if the dip for that distance is some 80 feet a mile e se then the thickness of the Marcellus and Hamilton formations is 2025—340 feet which equals 1685 feet. he ay XXVIII C. From West Fulton a section was followed up was G | ther creek to its head in the western part of Fulton township ee ee _and there are also layers of blue fiagging stone of fair ich | Some of the rather irregular sandstones contain numerous Ba meng of Spirifer granulosus (Con.) H. & C. associated with other Hamilton species. The quarry’s elevation above Panther creek — at West Fulton was not determined, but it is clearly several - hundred feet below the top of the Hamilton formation in the — lower part of the zone called C! of this section. oes a Three and one fourth miles w n w of West Fulton in schnar a ies district no. 7 the main branch of Panther creek turns sharply — tea to the north; but the section follows the highway toward Sum-_ mit and the smaller branch of the creek up the hill to the west. ~ Some 490 feet higher than West Fulton, on the south side of the road after crossing the west branch of Panther creek and passing the road on which the schoolhouse is located, are quite thin, bluish, argillaceous shales (C*) certain layers of which con- tain abundant specimens of the very mucronate form of Spirifer’ 4 mucronatus (Con.) Bill. associated with Chonetes coronata (Con.) . aye Hall. These shales are clearly in the Hamilton formation. The 2 following species were collected: 1 Chonetes coronata (Con.) Hall 2 Spirifer mucronatus (Con.) Bill. Sa ee eae 3 Cyrtina hamiltonensis Hall (rr) ee 4 Camarotoechia congregata (Con.) H. & C. (rr) 5 Macrodon hamiltoniae Hall (?) ro (rr) Imperfectly preserved. 6 Orthonota undulata Con. — | (rr) ‘ 7 Prothyris lanceolata Hall | | (rr); 3% 4 CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 191 ‘For 50 feet the hillside is covered when another outcrop of ~ coarser and more arenaceous shales (C3) is reached which also con- . \ tains abundant Hamilton fossils. The shales are capped, by very thin bedded, even sandstones and the zone is clearly in the Ham- ~ ilton: 1 Spirifer granulosus (Con.) H. & C. (rr) Oe audaculus (Con.) H. & C. (c) 3 Camarotoechia congregata (Con.) H. & C. (c) 4 Pterinea.flabella (Con.) Hall | (rr) 5 Liopteria bigsbyt Hall (?) (r) Broken and poorly preserved. On the hillside 55 feet above C*, or approximately 595 feet higher than West Fulton, are thin, bluish gray sandstones (C*) In which a few fossils occur. This ledge is about on a level with the small cemetery on the north side of the road, and is appar- ently in the Hamilton formation. 40 feet higher is a ledge of thin bedded, bluish gray sandstone five feet in thickness. A lit- tle below this stratum are loose fossils which seem to have come He from this outcrop and apparently show its Hamilton age. At the edge of the woods on the south side of the road are ledges of rather coarse grained, thin bedded, grayish sandstone (C%). © There are from 15 to 20 feet of these sandstones exposed, which apparently occur on the north side of the road at a little higher elevation. No fossils were found except plant stems; but there are numerous clay pebbles in some of the layers. This zone is probably near the dividing line between the Hamilton and Sher- burne formations and it is a matter of some uncertainty to which formation it should be referred. On the highway 50 feet higher or 825 feet above West Fulton are bluish to greenish ar- gillaceous shales (C) and bluish gray flagging stone. No fossils were found and in lithological characters these rocks closely resemble those of the Sherburne formation to which they are referred. Just south of the turn on the first road turning south toward Eminence are thin bedded, bluish gray, flagging stones (C*) below which are smooth, bluish, argillaceous shales weather- ing to an olive tint and containing some concretionary nodules. These shales are about 45 feet above those of C°. _ On the highway one and one fourth miles east of Summit, in the eastern part of Summit township, on the divide, is a layer of rather irregular sandstone (C*) which contains a few fossils. “NEW ‘YORK STATE 1 MUSEUM é _— (192 There are also fossils in bls argillaceous shales _ just above the a On each side of the summit : Desrsiiuiis Hall. The list of fossils is.as follows: 1 Spirifer mucronatus (Con.) Bill. DAS: tullius Hall ; : 3 Tropidoleptus carinatus (Con.) Hall _ 4 Microdon (Cypricardella) bellistriatus Con. 5 M. (C. ) gregarws Hall 6 Sphenotus cuneatus (Con.) Hall 7 Schizodus OREO (Con.) Hall branches of the Westkill are coarse, grayish sandstone and thinner blue shales (C’—). This ledge is 140 feet lower than | the fossiliferous zone of C8 and is propably near the top of ee is Hamilton. Fossils occur rather sparingly, the three following species having been collected during a few minutes search: ; be 1 Tropidoleptus carinatus (Con.) Hall / 2 Spirifer sp. Fragments. 3 Nuculites oblongatus Con. Large specimen—35 mm long and 19 high. , On the western side of the divide going down into the second valley, sandstone and coarse shales containing abundant Hamil- ton fossils were found 120 feet below the zone C%. Between the ee two fossiliferous zones are exposures of sandstones and smooth — bluish to olive shales which closely resemble, lithologically, those of the typical Sherburne formation. Teo the north of the road | and northeast of Summit is a high, rounded hill, known as Cob- : ble hill, on which are plenty of these fine shales, the Sherburne formation apparently capping the hill. - : re The section described above may be represented diagrammane 3 ally in the following manner: a a ‘ : ng # rs Awe 2 Pac ia ‘ ena iA 7g CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 193 SECTION UP PANTHER CREEK TO THE DIVIDE WEST OF WEST FULTON 950” 945’ 870’ 825’ 95 755! 595’ 540’ 490’ 0’ XXVIII C Divide on road 14 miles east of Summit O® Shales and sandstones containing fossils Ithaca C7 Bluish to olive shales and sandstones on Eminence road : Cé Greenish shale and thin bedded sandstone Sherburne C® Thin bedded, grayish sandstone Covered Bluish-gray sandstone; loose fossils . Hamilton ¢* Thin sandstones with a few fossils C? Coarser Hamilton shales C? Fine Hamilton shales C1 Quarry 4 mile west of West Fulton Hamilton Panther creek at West Fulton 194 NEW YORK STATE MUSEUM. oe ale The elevations in the above section, although obtained by — means of a barometer, are considered fairly accurate for geo- logical purposes, since on comparing the elevation of a certain horizon of this section above sea level with that of Summit hill whose altitude was determined by the New York survey under Gardiner it was found that the estimated altitude of the section was only 70 feet too great. In estimating the altitude of the section above sea level Guyot’s elevations of the Schoharie val- ley were used? which were obtained by means of a mercurial barometer; while from the mouth of Panther creek to the top | of the hill east of Summit, the measurement was made by means ~ of an aneroid. | ma oe On comparing the altitude of the fossils found at XX VIII C?— oo which are thought to come from about the top of the Hamilton, nig with that of the highest Hamilton zone in the Summit hill section it is found that the Summit fossils are 300 feet higher, or 370 feet if the correction mentioned above be made. The distance between the two localities is two miles which gives a dip of from 150 to 185 feet a mile to the southeast. If the above calculation be correct and this strong southeasterly dip con- tinues to the Schoharie river, then the thickness of the rocks’ - in any section continuing westerly for several miles based upon the altitude would be too great. This is probably the case for the one just described up the Panther creek from West Fulton and the altitudes of the section are greater than the thickness of the rocks represented in it. Blenheim Blenheim township lies to the south of Fulton and to the east of Summit and Jefferson. Its eastern part is crossed by the Schoharie river bordered on the east by a very steep hill which in places has almost perpendicular walls several hun- dred feet in hight. The central part of the township is crossed from the west toward the east by two streams known as the Westkill and Mill creek which unite near North Blenheim and @Am. jour. science, 3d ser., 19:449. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 195 enter the Schoharie river at that locality. Both of these creeks have cut deep valleys, specially in their lower courses. XXVIII V. This section begins near the level of the Schoharie river, two and one half miles south of Bouck’s falls, or about half _ the distance from Panther creek to North Blenheim, and follows the highway along the Fulton-Blenheim boundary to the north- west. Along the river road are smooth, bluish shales (V’) which contain very few fossils although they are shown by the overlying rocks to be in the Hamilton formation. Just above the first house on the road leading up the hill to the southwest in the southern part of Fulton township is an exposure of 15 feet of bluish, arenaceous, quite fossiliferous shales (V’), approximately 165 feet above the level of the river. The shales contain a Ham- ilton fauna in which formation this zone belongs and the follow- ing species were collected: 1 Camarotoechia prolifica (Hall) H. & C. (aa) Very abundant in thin layers. 2 Spirifer audaculus (Con.) H. & C. (2) (ri), Imperfectly preserved. 3 Ambocoelia umbonata (Con.) Hall (rr) 4 Strophalosia truncata (Hall) Beecher (?) : (r) 5 Paracyclas Wirata (Con.) Hall. (rr) ‘6 Orthonota (?) parvula Hall (rr) T Nyassa arguta Hall (rr) 8 Pterinea flabella (Con.) Hall (rr) 9 Actinopteria boydi (Con.) Hall (rr) A massive sandstone (V*) crosses the road 65 feet above the shales and runs along the highway to the northwest for some two and one half miles to a point near the first road turning to the north, the bed rock being mostly concealed by drift. Ac- cording to the barometer the top of this concealed interval is 595 feet above the massive sandstone of V3, although on account of the southeast dip as shown above, it is not probable that the concealed rocks have this thickness. Just below the first turn to the north -are ledges of rather thin bedded, coarse grained, grayish to bluish gray sandstone, 20 feet of which are exposed. 196 NEW YORK STATE MUSEUM No fossils were found. It is uncertain in which formation this — ledge belongs and on account of the great thickness of the con- cealed rocks it is impossible to indicate the approximate line of division between the different formations. For nearly 500 feet above the sandstone ledge of V® the bed rocks are largely eoncealed although there are occasioned exposures of sandstones. At this elevation, approximately 1350 feet above the level of the Schoharie river, the summit of this section is reached and the land is about as high as any in this general region except to the south where the spurs of the Catskill mountains are conspicuous toward Stamford. On the surface are large numbers of loose blocks of coarse grained, grayish sandstone but no pieces of red rock were seen. Some of the sandstone is of greenish oray color, similar in appearance to the Oneonta formation and like the sandstone which will be described later, near the top of the hill west of North Blenheim and four miles southeast of this locality. The general features are shown in the diagrammatic section — reproduced herewith. - About two and one quarter miles west of the summit of the above section is the village of Eminence on the western line of Blenheim and at the corners of Summit and Jefferson townships. To the east of the village and some 50 feet higher is a rounded highland which forms the top of section XXVIII V. Between the two hills is a deep and narrow valley formed by the main northern branch of the Westkill. Capping the ‘hill is a ledge of thin bedded, coarse grained, grayish to greenish gray sandstone, six feet or more showing in the outcrop. No fossils were found and the rock considerably resembles coarse layers seen in the Ithaca to the east of the Schoharie valley, or even in the Oneonta. Noa red rocks in the ledge or even loose pieces were seen. This hill is about two and one quarter miles southwest of the Ithaca shales of XX-VIII W’ and four and one half miles northwest of the coarse sandstone (XX VIII D’) which caps the hill to the west of North Blenheim. One barometric reading gives the summit of the Eminence hill as 1200 feet above the level of the Schoharie river 0 J CYOAMVYD HOFSN %j ees ‘ THUMLISAM WOU HOLON dagq CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 197 at North Blenheim, while the coarse sandstone D® west of North Blenheim is 650 feet above the river level. If these two zones represent about:the same horizon then there is a dip of approxi- mately 122 feet a mile to the southeast. XXVIII Dt. To the west of North Blenheim is a steep hill be- tween the Westkill and Mill creek. The rocks exposed in the gorge at the lower end of the Westkill and in the eastern end of this hill form an interesting section, passing from the Hamilton formation at the base to the coarse grained, greenish sandstones near the top similar to the Oneonta. In the Schoharie river at North Blenheim are coarse, grayish sandstones which do not closely resemble the Hamilton although they are probably in that. formation. Some 30 feet above the river is the foot of the gorge in the lower part of the Westkill at the falls. The sides of the gorge are perhaps 50 feet in hight and the rocks consist of sandstone alternating with shales of olive, blue and greenish color. In the blue and olive shales below the falls are numerous specimens of Paracyclas tenuis Hall, and (?) Beyrichia sp. is also common. This exposure resembles the Sherburne formation in lithologic appear- ance; but 25 feet higher are blue shales containing a number of Hamilton species so that it is perhaps better to regard this zone as one of the transitional beds from the Hamilton to the Sher- | burne formation. Mather mentioned the fossils at this locality stating that “ The gray grits by the falls at the tannery, at North Blenheim, contain fossil shells. They were first observed by Prof. Vanuxem, who found their stratum about six inches thick. Several localities were observed where many species of fine shells may be obtained, in the bluish and brownish gritty shales on the road from North Blenheim to Gilboa.’”@ Mather also indicated the top of the Hamilton on his section “up the valley of Schoharie creek ” as near North Blenheim and succeeded by the Portage group.2 This is about the same clas- sification as that indicated above, since the writer regards the aGeology of New York, 1843, pt 1, p. 322-23. Hibid., pl. 25, fig. 6. a] These fossils show that at this horizon the rocks of the Ithaca NEW YORK ‘STATE MUSBUM Wat aa ‘Sherburne formation of eastern New Sok as synchronous w _ the lower part of the Portage of western New York. is stones alternating bie blue, arenaceous shales, in Home of ‘a sy ae with a smaller number of specimens of other pee : The complete list is: | e 1 Tropidoleptus carinatus (Con.) Hall 2 Chonetes coronata (Con.) Hall (?) 3 Ambocoelia umbonata (Con.) Hall 4 Camarotoechia congregata (Con.) H. & C. One specimen resembles somewhat GO. stevensi (Hall) H. & C. me) Cephalopod Fragment of shell. > > tas soe Westkill gorge and shows the transitional nature of the bee in the lower part of this section. meh XXVIII D*. In ascending the eastern ean. of the hill for Pee _feet above the shales by the highway the rocks are largely covered. At an elevation of 270 feet above the river level, however, are plenty of loose, angular shales which evidently came from a ledge — 6 rs. at about that horizon. These shales are quite fossiliferous con- taining a large number of specimens of Camarotoechia stevenst — (Hall) H. & C. and an occasional one of Spirifer mesastrialis Hall. group are reached. The complete fauna is: 1 Camarotoechia stevensi (Hall) H. & C. Very abundant in a thin rotten sandstone. (aa) 2 Spirifer mucronatus (Con.) Bill. (?) a ae mesastrialis Hall The fine striae are only faintly shown. 4 Sphenotus cuneatus (Con.) Hall : 5 Goniophora carinata (Con.) Hall 6 Modiomorpha sp. No.28, D. §L.CT/ON OL HILL BETWEEN MESTAUL SWULL CREEKS We OF N.BLENHEIM. 760 COARSE 6 REENISH- 6RAY SANDSTONE . FED SANDSTONE NEARLY IN PLACE, Base of HEAVY 6RAY sANosrone ONEONTA?) Seaces wirnssunoan7r Fossits /74ACA, (Spe ws fer weesastetolis ) SHALES FORMING BENGH, LAFCE Hhyn chonéllas SHAL Y SANOSTONE. MIAINLY COVERED. BY FOBROSIDE 2 SHALES WITH Ccepdoleptys AWD ti fynchoyclle WALES AND THIN SANOSTONES IN SHALES, RAULIOA IT CUPZL . River ltevyet ar W. BLEN HES mM. _ § QLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 199 7 Palaeoneilo cf. plana Hall ; (rr) 8 Lingula sp. (rr) 9 Grammysia cf. elliptica Hall (rr) Similar to the specimen from Ithaca, N; Y., as figured on pl. De, fe. 1. 10 cf. Glossites depressus Hall (rr) 11 Bellerophon SDan: 2 a tERy Fragment of a very large specimen showing a strong mesial band with a deep sinus at the front of the shell. 12 Tentaculites spiculus Hall (c) Another bench of shales occurs 310 feet above D? and at this horizon quite a number of species were collected from the loose pieces though it is not certain that all of them came from this zone. The list follows: . A Camarotoechia stevensi (Con.) Hall (?) 25 Ces 2 Spirifer.mucronatus (Con.) Bill. (?) . (rr) Poorly preserved. 3 8. mesastrialis Hall (r) Most of the specimens are worn and do not show the fine striae, but on the dorsal fold of one they are clearly shown. 4 8. Sp. ° (rr) In form and size of plications like Sp. granulosus (Con.) Hall, but too imperfectly preserved to show granules. 5 Crinoid stems. (r) . Segments of small ones. 6 Dalmanites (Crypheus) boothi (Green) Hall | (rr) 7 Microdon (Cypricardella) tenwistriatus Hall (rr) 8 Nyassa arguta Hall es Same at least as fig. 7 and 8, pl. 53, from Pitcher Springs, which is in the Ithaca group. 9 Sphenotus truncatus (Con.) Hall (c) These range from 10 to 20 mm in length and are apparently quite good specimens of this species. 10 Goniophora hamiltonensis (Hall) Miller (?) (r) Not clearly preserved but apparently this species. 11 Palaeoneilo constricta (Con.) Hall var. flecuosa Hall (rr) 200 NEW YORK STATE MUSEUM 12 Leptodesma cf. rogersi Hall The specimens being poorly preserved do not show the spine and do not seem to be quite so oblique on the umbonal ridge. 13 (2) Schizodus sp. | ~ (er) Badly broken. 14 Liopteria dekayi Hall (rr) 15 Orbiculoidea sp. | (rr) Broken and poorly preserved. On the supposition that this zone and that of XX VIII X® on the hill south of West Fulton are at about the same horizon, near the base of the Ithaca formation, a calculation was made which gave a dip of 174 feet a mile to the south southwest. Again the same — calculation was made between this zone and that of XXVIII C8 on the hill east of Summit which gave a dip of 129 feet a mile to the southeast. | It will be noticed that this dip of 129 feet a mile agrees very closely with that obtained for the sandstone of the Eminence hill and D® of this section which is 122 feet. The general agree- ment of these several localities seems to demonstrate that this portion of Schoharie co. has a considerable southeast dip. | XXVIII Dt. A ledge of rather thin shales in which fossils are abundant occurs 640 feet above the level of the river. Spirifer mesastriaiis Hall and other species of the Ithaca formation were found and the entire list is as follows: 1 Sphenotus cuneatus (Con.) Hall (c) 2 Orthonota undulata Con. (rr) 3 Schizodus appressus (Con.) Hall (?) ! (c) Rather smaller though near the form of this species. 4 Grammysia (Sphenomya) cuneata Hall (rr) 5 Leptodesma rogersit Hall (c) 6 Lnopteria dekayt Hall i (r) ae, Sp. | (ee fine concentric striae. 8 Spirifer mesastrialis Hall (r) | 9 Lnorhynchus mesacostalis Hall (?) (rr) 10 Orbiculoidea sp. | (rr) 11 Tentaculites sp. i (r) CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 201 | XXVIII D>. Only 10 feet above this terrace of the Ithaca shales is a ledge of gray, coarse grained, thin bedded sandstone with the lithologic appearance of the Oneonta. 20 feet above its base red sandstone was found which was thought to come from a stratum at about that horizon but perhaps this is not the case. There is, however, some positive support for the supposition that this red sandstone is nearly in place since at Gilboa in the Schoharie river are red sandstones and shales which according to Sher- wood’s section are 666 feet above the gray sandstone which makes the rapids in the river at North Blenheim® ; while the red sandstone on the hill west of North Blenheim is approximately 670 feet above the same horizon. 90 feet above the red sand- stone is a cliff of massive coarse grained, greenish sandstone, forming the eastern end of the hill, at an altitude of 760 feet . above the river level. This sandstone in its lithologic appear- ance closely resembles the Oneonta although it probably occurs. at a lower horizon than the sandstone farther west in Jeiferson township which has been called the base of the Oneonta forma- tion. : XXVIII H2. This section follows the highway from North Blen- lieim toward Jefferson along the side of the steep hill to the north of Mill creek and is nearly parallel to the section just de- scribed. The exposures for the lower part of it are about the same as those for XXVIII D, above which the rocks are covered for a considerable thickness, and this part is called Ht. At 440 feet above the river a heavy bedded, quite coarse grained, mas- Sive, greenish gray sandstone is reached (H), 30 feet of which is shown in the highway and this is succeeded by 35 feet of greenish and bluish, smooth, argillaceous shales (H?). No fossils were found either in the sandstone or the shales. The eleva- tion of this sandstone, 440 feet above the river, agrees closely with the thickness of 431 feet assigned by Sherwood to the rocks from the rapids at North Blenheim (formerly Patchin Hollow) to the coarse gray sandstone which forms the top of the Little el a Proc. Amer. philosophical scciety, 17:347-48. 202 NEW YORK STATE MUSEUM Manorkill® (this is supposed to be the falls generally called thes ae _ Minekill). | 3 XXVIII H+. On top of the smooth, argillaceous shales of His a layer with pebbles making a sort of conglomerate in which fossils are common. Succeeding this layer are bluish, argil- — laceous shales which also contain numerous fossils. Some of the layers in the shale are somewhat calcareous, containing abundant specimens of T'ropidoleptus carinatus (Con.) Hall, and ie form a sort of fire-stone. These shales constitute one of the most fossiliferous zones found in the Ithaca formation and it is an excellent locality. for collecting. It will be farther seen on referring to the list of 42 species recorded from this zone that it is practically Hamilton and furnishes an interesting example of the recurrence of this fauna. Spirifer mesastrialis Hall was. not noticed in this zone, but in section XX VIII D this species was found some 235 feet lower and also higher. The fauna is interest- ing and richer than that found at any other locality. 1 Spirifer mucronatus (Con.) Bill. ; (a) 28: tulius Hall . (c) ae granulosus (Con.) H. & C. (r) 4 Tropidoleptus carinatus (Con.) Hall (a) . | 5 Athyris spiriferoides (Eaton) Hall — (c) 6 Chonetes setigera Hall. (a) | Cs coronata (Con.) Hall (r) 8 Cryptonelia (Hunella) lincklaent Hall . (r) 9 Palaeoneilo maxima (Con.) Hall | (c) AP? emarginata (Con.) Hall (rr). 11 Pholadetla radiata (Con.) Hall | (CG) pet 12 Nucula bellistriata (Con.) Hall (rr) 13 Glyptodesma erectum (Con.) Hall (c) 14 Orthonota wndulata Con. (r) 15 M odiomorpha concentrica (Con.) Hall (rr) 16 UM. mytiloides (Con.) Hall (rr) 17 M. subalata (Con.) Hall fi: _ var. chemungensis Hall (rr) aProc. Amer. philosophical society, 17:347-48. NakE,4.SLECTION ALONG MILL CRELA From NV. QLENKEIM TowAROUEFFERSON, V29 Sunmmir oF ROAD. ConRsé 6REENISH-6RAY SANOSTONE LOOSE ON SUAFACE. No0.kE.Z. SECTION ALONG MNEMULL CALE ONEONTA KZ ; Aurea Cxvercn L00SE HEAVY 6FEENISH-GARAY CANISTONE 235.) 650) Alosrey COVERED, BUT LEOCbES OF COARSE SANDSTONE. Z SS YH47S| Mosriy covereo. {ze OWS ones . . NY AOA: S LOOSE BLUISH SHALY SANOSTOVE WITH FOSS/LS. MASSIVE EREENISH-64 44 SAN OSTONE. Zt | FA0 SANOSTONE AND MOTTLEO SHALE. PARTLY COVERED “ano PAATLY 4590 SLVE SHALES. Z* | 6Creenisn SHALES WITH Spéirtfer pruecaslereoLis, SLUISH AGILE ACEOUS SAALES 4 AES WITH ABLNOANT Fossits. /THAGCA. GREENISH AND BLUISH AR 6c ACEous |\F8F Waser Giz e0a, SHALES. HEANVVY-BEODEO 6REEN/IS H=- EFAY SANOSTAONE. GO| Laacecy Cove reo. z2 FINE BLVE SHALE WITH FOSSILS. /THACA COvERED : OCCASIOWAL EXPOSURES OF BLVE TO 6REENISH SANOSTONE, SHERBURNE BLuE MASSIVE SANOSTONE. Miné Hier FALLS. GLUE SHALE WITH AW OCCASIONAL THIN SANDSTONE. BLUSH SHALES wirh Few FOSSILS, /THACA LOweER PART SAME AS Wo. 28,0. LEVEL OF ScHOoHAARIE AIVEF. LEVEL OF SCHOHARIE RIVER ~ - 18 19 20 et o> 23 2A 25 26 ay 28 29 30 31 32 ats) 34 30 36 37 9 vo 39 40) 41 42 Goniophora hamiltonensis (Hall) Miller Imperfectly preserved. G. rugosa (Con.) Miller Nuculites triqueter Con. N. oblongatus Con. Grammysia subarcuata Hall G..- arcuata (Con.) Hall G. globosa Hall Actinopteria boydi (Con.) Hall A. decussata Hall Beilerophon acutilira Hall Crushed and imperfectly preserved. Coleolus tenuicinctum Hall . Phacops rana (Green) Hall Dalmanites (Crypheus) boothi (Green) Hall Orthis (Rhipidomella) vanuxemi Hall (?) Orthothetes chemungensis (Con.) H. & C. Chonetes lepida Hall Solen (Palaeosolen) siliquoidea Hall Microdon (Cypricardella) bellistriatus Con. (?) Imperfectly preserved. M. (Cypricardella) tenuistriatus Hall Macrodon hamiltoniae Hall ‘Cimitaria recurva (Con.) Hall Hyolithes aclis Hall Leda diversa Haii Cyrtolites (Cyrtonella) pileoius Hall Pleurotomaria rotalia Hall CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 203: (c) (rr) (rr) (rr) (rr) (rr) (rr) (rr) (rr) (r) (rr) (rr) (r) (rr) (rr) (r) (rr) (rr) (c) (rr). (rr) (rr) (rr) (rr) (rr) XXVIII H®. Succeeding these fossiliferous shales for 85 feet the rocks are partly covered; but there are not infrequent exposures of blue shales. Fossils were not found. The examination was hastily made and the shales are undoubtedly fossiliferous as are those of the same general horizon in XXVIII D* which contain speci- ments of Spirifer mesastrialis Hall. These blue shales show within 10 or 15 feet of the base ledges of coarse grained, irreg- ular, thin bedded, grayish to greenish gray sandstone (H°) which 204 «NEW YORK STATE MUSEUM weathers to a light gray color and resembles in lithologie appear- | . ance the Oneonta sandstone. The base of this ledge is barometri-_ %,.) me os cally 640 feet above the Schoharie river, which is only 10 feet lower than that of the similar ledge in section XX VIII D®. On the | surface not far above the base are loose blocks of red sandstone, — a but it was not found in place. Along the road to the west the ae rocks are largely covered on the high ground in the western part aes of Blenheim and. eastern part of Jefferson. But at the summit of the road in the eastern part of Jefferson there is plenty of the coarse, greenish gray sandstone loose on the surface and the long 14 lines of stone walls are constructed largely of it. In altitude fre this locality is barometrically some 650 feet above H® or 1290 oo feet above the Schoharie river at North Blenheim; but if there be ee a dip of 80 feet a mile to the south of east, as along Panther ee creek, then the thickness of the rocks would not ne more than 350 ee feet for this upper part of the section. XXVIII E+. By the side of the river road about one and one nie ag half miles south of North Blenheim and 345 feet higher are bluish, argillaceous shales which are fairly fossiliferous. They contain Re: a specimens of: ioe a me 1 Spirifer mucronatus (Con.) Bill. : (rr) ee 2 Chonetes setigera Hall \ OTe 5 Tropidoleptus carinatus (Con.) Hall : Pas sn ¥ a 4 Grammysia sp. (rr) Only fragments. XXVIII B'. On the eastern side of the Schoharie river below North Blenheim and in the northeastern part of the township is a My x Zz ‘= $ PLS - iF Ren Ny, CRN earn Tia! Ha AS ot 9 ee cee. oe PO ae ak Re ae precipitous wall of rock out of which the highway has been cut; a locality known as the “ dugway.” The rocks consist of soft, blue, argillaceous shales with thin layers of sandstone. The irregular layers of shales contain some rather poorly preserved fossils; but the smooth shales seem to be barren. Toward the top, of the cliff is a layer which has somewhat concretionary structure, similar to that noted in other localities in the upper pe 3 Hamilton and succeeding formations. This cliff is shown to be CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 205 in the Hamilton formation both by the fossils in the rocks on the western side of the river at XXVIII V2, which at 165 feet above the river are not far below this locality, and by those which occur in the shales. 1 Oamarotoechia prolifica Hall (a) Abundant in a thin layer. 2 Nuculites oblongatus Con. 7k) 3 Palaeoneilo constricta (Con.) Hall: (rr) 4 Phthonia sectifrons (Con.) Hall (rr) 5 Orthonota (?) parvula Hall (rr) 6 Pholadella radiata (Con.) Hall (rr) 7 Grammysia arcuata (Con.) Hall (ree 8G. lirata Hall (rr) 9 Pterinopecten vertumnus Hall (Cc). 10 Bellerophon patulus Hall (?) (rr). In the Schoharie river valley region the line of separation be- tween the Hamilton and Sherburne formations is not as clearly shown for part of the distance as it generally is farther west. This is due largely to the heavy mantle of drift covering the slopes of part of the hills, also the valley near North Blenheim where the characters of the two formations blend. It was shown pretty clearly, however, in Fulton township that the line of. division is well toward the top of the high hill south of Panther creek which is followed to the upper part of the high hill west of the Schoharie river. Then the line is along the side of this hill dipping quite rapidly to the south and reaching the river valley in the vicinity of North Blenheim and apparently crossing the river somewhat south of that village. Then it gradually rises on the slope of the hill east of the river as it is followed northerly till opposite Breakabeen we find it on the hill to the east and above Houston Corners. From there it continues northerly to the Moheganter hill in the southern part of Middleburg, enters. the northwestern part of Broome township and follows the western side of Catskill creek for some distance below Franklin- ton before it crosses to the eastern side. | olka wen | 2064.4. NEW YORK STATE MUSEUM . , Gilboa To the south and east of Blenheim is Gilboa which is the mid- dle one of the three southern townships of Schoharie co. The central part is crossed from the south to, the north by the Schoharie-river to the east of which, from a short distance below Gilboa village to beyond the northern boundary of Gilboa and Blenheim townships, a high and precipitous hill rises. The two other principal streams of the township are the Minekill, which rises in the eastern part of Jefferson township and enters the, ' Schoharie river from the west, and the Plattenkill from the east. XXVIII Z. About half way between the villages of North Blen- heim and Gilboa is the Minekill the lower part of its courserunning very near the township line. Just to the south of the Minekill along the western bank of the Schoharie river are bluish shales in which a few imperfectly preserved fossils occur. The rocks however are principally rather thin, bluish sandstones, ap- parently unfossiliferous and there is one prominent layer of green shales. The fossils from the blue shales near the mouth of a brook south of the Minekill are so imperfectly preserved and fragmentary that it is scarcely possible to identify them more than generically. The list as far as the specimens were deter- amined is as follows: ! 1 Liorhynchus (?) or Camarotoechia (?) sp. (c) The specimens do not seem to agree closely with the figures of the Ithaca species of either of the above genera. ‘2 (2?) Palaeoneilo sp. (rr) Broken specimen showing the characters imperfectly. 3 Orbiculoidea neglecta Hall (?) (rr) Specimen imperfectly preserved but apparently this species. 4 Lamellibranch : #:\ ie CEG Fragment of long shell in which the Discina is imbedded. In the Minekill just below the main river road are the cascade ‘and gorge known as the Minekill falls. The gorge at the cas- cade is very narrow and the. walls are perpendicular, perhaps 100 feet high. The main part of it is cut out of a sparingly fossilifer- CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 207 ous blue shale which contains an occasional thin layer of sand- stone. There are also thin layers of small, iron stained concre- tions and at the lower end of the gorge are some greenish shales. It is probable that these rocks are in the Ithaca formation al- though the list of fossils given below does not furnish very con- elusive evidence for Spirifer mesastrialis Hall was not found. 1 Tropidoleptus carinatus (Con.) Hall (c) 2 Spirifer mucronatus (Con.) Bill. (c) 3 Chonetes setigera Hall (c) 4 Orthothetes chemungensis (Con.) H. & C. (?) (rr) 5 Nuculites oblongatus Con. (rr) 6 Leda brevirostris Hall (rr) T Lunulicardium fragile Hall (rr) ‘At the brink of the upper cascade and on the banks of the creek above is a blue, fairly massive sandstone containing Psilophyton princeps Dn. and other plant stems. XXVIII Z2. By the side of the road toward West Gilboa and about west of the Minekill falls are fine blue shales which are 365 feet or more above the level of the Schoharie river and below them are some quite heavy sandstones. The shales are fairly fossilifer- ous and are in the Ithaca formation. The following species were collected in a few moments: 1 Nuculites oblongatus Con. (?) , (rr) Posterior part missing. 2 Tropidoleptus carinatus (Con.) Hall . (rr) 3 Spirifer tullus Hall (c) 4 8. mesastrialis Hall (?) ey ‘Poorly preserved. 5 Lamellibranch shell. Imperfectly preserved. XXVIII Z?. On the Minekill four miles west of the Schoharie riveris the little hamlet of WestGilboa or Shoe Hollow. The rocks along the highway from Z? to this place are well covered, with only mow and then an outcrop of a sandstone stratum or a little shale. On the hill one fourth mile north of West Gilboa are greenish shales in which Spirifer mesastrialis Hall is abundant. The fol- lowing species were obtained: 208 _ NEW YORK STATE MUSEUM - 1 Spirifer mucronatus (Con.) Bill. p ASE Sh mesastrialis.Hall Thin layers nearly filled with these shells. 3 Tropidoleptus carinatus (Con.) Hall (ER 4 Microdon (Cypricardella) gregarius Hall (?) | (rr) Imperfectly preserved. E . 5 Palaeoneilo constricta (Con.) Hall (?) (rr) Imperfectly preserved. Only a few feet higher are ledges of thin red sandstone and mottled red and green shale (Z‘) approximately 590 feet above : the level of the Schoharie river. To the north of this hill about one mile from West Gilboa is Pigeon creek, a tributary of the Minekill from the north. Along the highway on the northern — bank of this creek as far as the first road are frequent pieces of sandstone containing fossils, frequently Spirifer mesastrialis Hall. These blocks were not found in place but it seems probable that they occur in place above the zone of reds described near West Gilboa. Higher on this hill forming the divide between the Minekill and Mill creek are large numbers of loose, angular, blocks of red sandstone. This seems to show that a considerable amount of the red occurs in this hill interstratified with the coarse grained, grayish to greenish gray sandstone. Mixed, loose specimens of these two colored sandstones occur well toward Ruth church which is on the high part of the divide in the south- western part of Blenheim, 475 feet by the barometer above the red sandstone north of West Gilboa. Not far from Ruth are large quantities of loose, angular blocks of greenish gray sandstone similar to the typical Oneonta. Loose by the highway about one fourth mile west of West Gilboa are blocks of greenish sandstone containing Ithaca fossils some of them having large numbers of Spirifers. It is not clear whether these blocks came from a hori- zon below or abovesthe red sandstone of Z*, but the following species were collected from them: 1 Spirifer mesastrialis Hall (rr) Two broken shells. é 7A mucronatus (Con.) Bill. (?) (rr): Two fragments and one small specimen. ay a4 . + cs: . f ede Box: ~ / - CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 209 3 Microdon (Cypricardella) gregarius Hall 2 (rr) 4 Nuculites cuneiformis Con. (?) (rr) Shell imperfectly preserved. 5 Palaeoneilo sp. | (r) Heavy concentrie markings like P. emarginata (Con.) Hall; . but there is no constriction... Something like the shells found in the Ithaca in N. H. Pennsylvania. Not far west of West Gilboa loose blocks of red sandstone occur frequently along the highway, but a ledge was not seen in place. In fact there are but comparatively few exposures of rocks in place along the upper course of the Minekill. Some two and one half miles above West Gilboa loose blocks containing fossils were seen by the highway, but it is not certain that they came from that immediate vicinity. In these blocks the follow- ing species were obtained: 1 Spirifer mesastrialis Hall Page (rr) 2 Homalonotus dekayi (Green) Emm. (?) (rr) 3 Paleoneilo emarginata (Con.) Hall var. (c) The posterior emargination, as in Pennsylvania specimens, is not as deep as on typical specimens of this species. 4 Microdon (Cypricardella) sp. Too imperfect for specific identification. LXXV Et. On the western bank of the Schoharie nearly two miles below Gilboa where the road runs very near the river are massive unfossiliferous sandstones which are fairly coarse grained and mostly gray in color with but a faint tint of green. Perhaps one fourth mile belowthe Gilboa bridge near the bank of the river is a small quarry E? which has been worked to some extent for building stone. The rock is a massive, rather coarse grained, greenish gray sandstone which runs down to river level, some 20 feet being exposed. No fossils were found in the bed rock; but on the stone wall aiong the highway at this locality are large ; blocks of bluish sandstone containing specimens of T’ropidoleptus carinatus (Con.) Hall; Spirifer sp.; Glyptodesma erectum (Con.) Hall and other fossils. Careful search was made for this zone in the vicinity of Gilboa but without success and it is probable that the specimens came from the drift. Along the highway from Grint Pera DIE CAN co ed ae TA Beir Past ene re ae gh MMT AZ! y igh ey TH ig ie Ah . I 1 k 4 rit = io eae ; _ NEW YORK STATE MUSEUM ee ee BS) to Gilboa. the soil as eunenas quite reddish inateme the ; nearness of red rocks. Above and below the highway bridge « ihe Schoharie river at Gilboa is.a rocky gorge (E*) with walls 5 ee and sandstones. The Rey ihe in seneny are coar Bee of the blocky, greenish shale by the roadside below the bridge Be a are fish scales. From the bridge for several rods up the stream | i We along the bank not much above the water is a stratum of | ove ie brownish red, silicious sandstone, nine inches in thickness. The : i . Jower part of the stratum is of a reddish green color, On the : o: + bank above the highway just south of the bridge is a stratum of | ‘ “ hee heavy, coarse grained, gray sandstone which contained the trunks sof the tree ferns, Psaronius textilis Dn., which were exposed Db: . mh the freshet of September 1869. Several of the trunks were secured by Prof. Hall and are now in the state museum of natural history ‘ ae Prof. Hall described at an early date® the circumstances attend- : ing their discovery and submitted them to Sir William Dawson for description.o The impression of the side of one of thea trunks still shows very clearly i in the sandstone at this locality. . ; - LXXV B1 On the eastern bank of the Schoharie one mile below | Gilboa is a steep cliff rising very abruptly from the river. ie og rocks consist of massive greenish sandstones alternating ae greenish and blue argillaceous shales. The dip is from 1° to 13° S 50° E. In the river near the bank are large blocks isk greenish sandstone, similar to the stone in the quarry on the western bank farther up the stream. On one of the largest. blocks which did not appear to have been transported far wal the a 24th an. rep’t N. Y. state museum of nat. history, 1872, p. 8, 15-16. ; b Quarterly jour. geol. society—London, 1871, 27:269; and Geol. surv. Canada, the fossil plants ai the Devonian and Upper Silurian formations of Canada, 1871, p. 59. ; > “e M SMe epee TNE ee] ADE ie OUR RM iat RE Hal Ba aK” ae ents eae ee gee ; tae | Ie Aare ie ate PP 7 Bat Vee AY: ary by AS a Ls } ¢ YS, or at A ri CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 211 river, are a number of good specimens of Amnigenia catskillensis (Van.) Hall, the characteristic fossil of the Oneonta sandstone. LXXV F. One mile above Gilboa the Manorkill enters ihe Scho- harie river from the east. Only a short distance from its mouth are the Manorkill falls, or cascade, which occur in a pretty glen that is quite a popular resort for picnic parties during the summer. The aecompanying picture gives a fairly good: idea of the falls. Below them reaching to the level of the Schoharie river is massive greenish gray sandstone with the lithological appearance of the Oneonta. According to Sherwood’s section” the base of the cascade is 57 feet above the top of the sandstone which contains the tree ferns, Psaromus textilis Dn., at Gilboa. Above the bridge there is a small fall above which on the southern bank of the creek are bluish to greenish crumbly shales containing fish plates one of which was recognized by Dr Eastman as probably belonging to Bothriolepis minor Newb. The number of specimens is not great and the fossiliferous layer apparently does not have any con- siderable extent. A few feet above are red shales forming a well marked zone in the sides of the glen, 12 feet in thickness. The rocks have a thickness of 120 feet from the foot of the cascade to the base of this zone of red shale as measured by Sherwood. The dip in the glen above the bridge varies somewhat with dif- ferent strata, but is decidedly to the southeast. On the northern bank it ranges from 1°-34°; while on the southern bank a dip of 14° almost directly east was noted. Several small specimens of Psaronius textilis Dn. were found by the side of the highway when this locality was first visited, which apparently came from some of the greenish gray sandstone when the excavations were made for the foundation of the bridge. At the saw mill one quarter mile above the mouth of the Manorkill and 200 feet above the level of the Schoharie river are © red sandstones and shales, 12 feet of which are exposed. Be- tween. the two zones of red shale there are some 56 feet of grayish sandstone and shale shown along the bank of the creek. This a Proc. Amer. philosophical society, 17:347. NEW YORK STATE MUSEUM upper zone of red shale was supposed by Sherwood to be ee cf same bed as the one of red and green shale in the pe ereek above the upper end of Palenville.¢ ee vis On the Geologic map of New York, published in 1844, the. top aa Be the Chemung rocks was represented as crossing the Schohariase 4 Se. river at the mouth of the Manorkill, and the Chem was suc = ceeded by rocks then considered Catskill. The rocks in the vicinity of Gilboa, specially at the Manorkill were quite well is i described by Emmons who correlated them with coarse sand- Ue stone found near Mt Upton and now known as the Oneonta sand- stone. The rocks at the Manorkill and vicinity succeeding those ce < in the more immediate neighborhood of Gilboa were described as follows by Emmons, “An undefined mass of gray sandstone ~ succeeds, which contains land vegetables, and, at the Manorkill falls, one mile above the village, also contains numerous fossils, — among which are several Cypricardia two species of Solen and. what appears to be the Terebratula lepida. The rocks are coarse ~ grits at the falls, with some layers of green tough shale, in which — wat . ¢ are contained most of the Cypricardia. The tough, lumpy char- acter of this shale is a great inconvenience to the collector of — fossils. Above the Manorkill falls, the red marl or slate is many — feet thick. This is succeeded by the greenish and coarse sand- stone shales alternating for five or six hundred feet,and appearing i in high and steep escarpments on the mountain half a mile north of the kill; the rock contains a few Cypricardia. The whole series” is fessiliferous; more so, we think, than what appears upon a cursory examination, principally on account of the coarseness of the grits and the unfavorable state of the stratification. The beds at and immediately above the bank of the creek near the village are destitute of animal remains, or at least we did not — succeed in finding any. Now the stratum which contains vege- — tables at other places contains also Cypricardia. In this stratum, many fragments of stems and long leaves are preserved, but crushed, and so broken that they are worthless as cabinet speci-- mens, yet the stratum itself is a good guide for the rock. It is. a Proc. Amer. philosophical society, 17: 347. Plate 12 MANORKILL FALLS, GILBOA - CLASSIFICATION, ETC. OK HAMILTON AND CHEMUNG SERIES 213 _the same as that described in Mr Vanuxem’s report, in which’ he first discovered the fossils at Mt Upton on the Unadilla. The discovery of this stratum (or strata, for there are several) at Gilboa, at the base of adjacent mountains, identifies two distant Series, and proves their equivalency and age... It has been said that the rocks of Gilboa belong to the Hamilton group, and as fossils closely resembling those of this formation were dis- | - covered six or seven hundred feet at least above the locality on. the Manorkill, where Devonian fossils had been found, it became important to accumulate as many facts as possible which would bear upon the question ; and we were fortunate enough to dis- cover the remains of fish in the strata between Prattsville and Gilboa, and, what was still more satisfactory was their associa- tion with the Cypricardia catskillensis [Amnigenia catskillensts (Van.) Hall] discovered by Mr Vanuxem, on the Unadilla. These fossus will undoubtedly be found quite numerous in this neigh- borhood, as we observed several specimens in the rock two miles above Prattsville, on the banks of the creek. It appears, there- fore, that it has a wide range in this series, and may be regarded as characteristic of the formation in which it is found.’’@ Darton states that the Oneonta formation ‘ begins at the Manorkill falls and extends about 12 miles southward ”’®; while on the Geologic map of New York the red shales in the gorge above the highway are apparently considered as marking the bottom of the formation. | : On the geological map accompanying this report the writer has — accepted for the base of the Oneonta formation from the Schoharie valley eastward, the lowest thick beds of red shales and sand- stones accompanied by coarse greenish gray sandstones. ‘These red rocks are not considered as marking the same horizon from this valley eastward, for the evidence seems to the writer to clearly show that the reds appear at a lower horizon as they are followed into Albany and Greene counties. The lowest reds, however, seem tc be about the only zone that can be followed for the purpose @ Agriculture of New York, 1846, 1:195-96. 6 Amer, jour. science, 3d ser. 45:206. Ve NEW YORK STATE. MUSEUM ~ of geological mapping and iets that a been taken for tke base of the Oneonta formation. 3 Along the Schoharie valley there is an ceeoad of the > Titho- logic characters and faunas characterizing the Ithaca and — Oneonta formations for several hundred feet. In the oa : specimens were rest in large blocks of this sandstone ee bank of the river which probably came from these sandstones. __ Considerably higher above these red and greenish gray sand. - >? stones a meager Ithaca fauna was found at several places in the Schoharie and Manorkill valleys. It was not satisfactorily | determined whether these highest fossiliferous layers occur ata higher stratigraphic position than the top of the Ithaca fauna in | oy the Susquehanna valley, but it is clear that the lithologic con- ditions of the Oneonta formation appear at a lower stratigraphic position in the Schoharie than in the Susquehanna valley and that | there is an alternation of these conditions through a thickness of several hundred feet of rocks. The Schoharie section is along ! the region of oscillation, between the marine waters with ‘They Ithaca fauna of the west and the brackish waters of the east. In the Susquehanna valley during this time, marine waters pre vailed as shown by the faunas, and there is no evidence of the | ‘brackish waters; while in Albany and Greene counties the brack- 3 ish waters dominated and there is scarcely any evidence of pe. Be faunas. | ; ae € -LXXV Al. This section extends from the Schoharie river at the Gilboa bridge along the highway toward Grand Gorge for more than one mile, and then to the top of the hill about south of Gilboa. | It is an especially interesting one since it shows the presence oft a fauna with a considerable number of species, over 400 feet oe above the river level and the first stratum of red rocks at Gilboa. a “The lower part of the section (A‘) is pretty well covered, but there ee are some outcrops which give.a general idea of the lithologic char- acters of the rocks. At-:the base are massive sandstones, above em oy, Plate 13 Ce eee aie MANORKILL FALLS ABOVE THE BRIDGE ‘CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 215 the stratum of red rock in the river gorge, which are coarse grained and grayish or greenish gray; then there are greenish shales followed by reddish sandstone. Higher are greenish and bluish shales and sandstones, and about 200 feet above the river level is the top of another zone of red shales. LXXV A*4. By the side of the highway toward Grand Gorge near the southern line of Gilboa township,375 feet above the Scho- harie river at Gilboa, are grayish to greenish gray non-fossilifer- ous sandstones alternating for about 15 feet with thin layers in which fossils are very abundant. The most abundant species is © Spirifer mesastrialis Hall, and these shells are so numerous that the layers form a sort of fire stone. These are succeeded by some 30 feet of greenish gray, thin bedded sandstones (A%) at the sur- face which at a greater depth form massive layers that are some- what irregularly bedded. The dip as measured by the ledges at the side of the road varies from a little less to more than 2° 8, 50° W. There is an occasional fossil in these sandstones as well as some clay pebbles. Below a ledge of massive, irregularly bedded sandstone are bluish, rather thin, argillaceous shales. These ' rocks make a prominent ledge in appearance, not unlike certain sandstones in the Oneonta formation. At the top of these sand- ue stones, 420 feet above the river at Gilboa is another fossiliferous zone, (A*), having the lithologic appearance of the lower one and containing abundant specimens of Spirifer mesastrialis Hall. From zones A? and A‘ the following species were collected: 1 Spirifer mucronatus (Con.) Bill. (r) 248) mesastrialis Hall (aa) Very abundant in these thin layers. 3 Camarotoechia eximia Hall (c) 4 Tropidoleptus carinatus (Con.) Hall (a) 9 Palaeoneilo emarginata (Con.) Hall var. (r) 6 Microdon (Cypricardella) complanatus Hall (rr) 7M, (C. ) gregarius Hall (rr) 8 Actinopteria boydi (Con.) Hall (r) 216 NEW YORK STATE MUSEUM 9 Pterinopecten cf. Vertumnus Hall (rr) < 10 (?) Nuculites sp. (rr) . 4 Large specimen in shape somewhat like WN. cuneiformis (Con.) though considerably longer and showing concentric. striae. These fossiliferous layers are apparently in the same general © stratigraphic position as the loose fossils found on the hil! north ,of West Gilboa toward Ruth and in the hill northeast of Gilboa which will be described after this section. They are clearly © above the zones of red shales shown in the gorge above the Manorkill falls and about 200 feet above the lower one. Suc- ceeding zone A‘ for 310 feet to the top of the hill 730 feet above the base of the section the rocks are partly covered, but there are frequent exposures showing an alternation of grayish sandstones with red shales and sandstones. The thick- ness and alternation of these rocks are shown on the accompanying diagrammatic section and their lithological characters agree either with those of the Oneonta or 2 Catskill formations. No fossils were found above A* except trails of worms on a loose specimen of grayish sandstone. The accom- panying “ Geological section along the Schoharie river from Scho- | harie to Gilboa”’ is intended to give an idea of the topographic outline of the hills to the west of the Schoharie river as well as the order and extent of the formations. On account of the lack of a topographic map of the Schoharie valley region it was diffi- cult to represent this section with any great accuracy and it is to ~ be regarded as a somewhat generalized section. It is thought, however, that it will give an impression of the rugged nature of this region and a somewhat graphic representation of the several formations which have already been described. LXXV O!2. About-one mile below Gilboa the Plattenkill or Flat creek enters the Schoharie river from the east. Between this creek and the Schoharie river is a high hill with a very steep bank toward ‘the river. On the southern end of this hill to the west of the Plattenkill and one and one half miles northeast of Gilboa are greenish gray massive sandstones (O+) while in shales La Fe bth » oe SS Rey i eos x N0.135 ,A.ELCT/0N OF fFIILL SM CHL, TOP OF Wee. AEO THIN-BFEOUED SANDSTONE. Covereo GRAVISH SAW OSTONE. COovERED. FEO SHALE CovEFE d, CRAyISH SAN OSTONE Coveren FEODISH SANOSTONE. Covered. FE ODISH SANOSTONE, Covered. UPPER ZONE OF FOSSILS. CovERE o. ZOWE OF FOSSILS. Lowesr Foss/Ls. AED SHALES GREENISH AND BLUISH SHALES AND SANDSTONES. BE DOISH SANDSTONE AWO SHALES, GREENISH SHALES. FE ODISH SANDSTONE GREEN/SH-6RAY MASSIVE SANOSTONE, @/LE0A BRIDEE OVER ScHoHAR/E£. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 217 (02) above the sandstones are fossils, Spirifer mesastrialis Hall being abundant. This species is associated with some others and in the few minutes spent in hunting for fossils at this locality the following list was obtained: 1 Spirifer mesastrialis Hall . (a) 2 Tropidoleptus carinatus (Con.) Hall (rr) 3 Camarotoechia sp. - (2) Too imperfectly preserved for specific identification. 4 Goniophora cf. hamiltonensis (Hall) Miller (rr) 5 Actinopteria boydt (Con.) Hall (er) ae In the massive sandstones below the fossiliferous shales Amnt- genia catskillensis (Van.) Hall occurs, which is considered the: characteristic fossil of the Oneonta sandstone. Below the mas- sive sandstones on the hillside are numerous loose pieces of red shale and sandstone. This fossiliferous zone is some 600 feet above the Schoharie river at Gilboa and clearly above the lowest zones of red shale in that vicinity and at the Manorkill. The lithologic character and fauna of the massive, greenish gray sand- stones (O*) are those of the Oneonta formation, while the shales of O? contain an Ithaca fauna similar to that of zones A? and A4 to the southwest of Gilboa. A dip of about 90 feet a mile to the southwest would carry the zone O? down to the horizon of A? which is between two and one half and three miles farther southwest. LXXV X?*. An interesting section was studied farther northeast . on the Mackey farm to the west of the Plattenkill. This locality is about two and three quarters miles northeast of Gilboa and the Plattenkill at that locality is some 550 feet higher than the Schoharie river at the mouth of the creek. On the Mackey farm 140 feet higher than the creek is a ledge of uneven bedded, gray- ish and rather coarse grained sandstones. 20 feet higher or ap- proximately 710 feet above the Schoharie river are thin bedded, grayish sandstones (X*) which contain quite a number of species, Spirifer mesastrialis Hall occurring abundantly. The fauna is as follows: the three faunas of LXXV A? 4, O? and X? and that the species « is reached at the top of the hill, approximately 900 feet above ie! Goes mesastrialis FAY fig Se ( 2.8. mucronatus (Con.) Bill. (2), 3 Tropidoleptus carinatus (Con.) Hall 4 Camarotoechia stevensi (Hall) H. & ©. we Poorly preserved. 5 Nucula corbuliformis Hall 6 Leda diversa Hall 7 Gonophora carinata (Con.) Hall 8 Coleolus aciculum Hall — 9 Microdon (Cypricardella) complanatus Hall ME UE (C. ) gregarius Hall 11 Actimopteria boydi (Con.) Hall 12 Pterinopecten suborbicularis Hall (?) It is to be noted that Spirifer mesastrialis Hall is abundant Brachiopoda are nearly the same in the three lists. ferent horizons, but the writer inclines to the former opinion. ‘a feet above X? are thin, gray sandstones eight feet in thicknes but no fossils were found in this ledge. Then for 117 feet the ‘ rocks are concealed when another gray ledge of thin sandstones — the Schoharie river level. The details of this section are shown Ps in the following diagram. EAST OF GILBOA LXXV Dy eS Thin gray sandstones at pe of hill Ps Plattenkill at the Mackey farm uM - ‘Schoharie river level 220 NEW YORK STATE MUSEUM Mackey’s Corners are reddish sandstones which are two and four = i tenths miles northeast of the Mackey farm and some 70 feet higher 4, “i than the fossiliferous zone of X2. Along the highway near the : head of the Plattenkill, east of Mackey’s Corners-and the school- house of district no. 18, are bright red shales and sandstones. This locality.is one and two tenths miles northeast of the one just de- scribed and approximately 190 feet above the fossiliferous zone — os of X?.. LXXVN. On the high plateau some two miles southeast of ) North Blenheim on the road turning south toward the Plattenkill =— from the old “state road” are conspicuous exposures of red shales (N41) which are approximately 1160 feet higher than the Schoharie ¥ river at North Blenheim. About one half mile farther south by ; the side of this highway are loose, bluish sandstones (N?) which * weather to a slightly olive tint and judging from their angular form evidently came from that immediate vicinity. These sand- stones are 115 feet above the red shales of N! or approximately 1275 feet higher than the Schoharie river at North Blenheim and about three miles north of the fossiliferous shales O? at the south-. ern end of this hill. Fossils are quite common in them, specially Spirifer mesastrialis Hall and Actinopteria boydi (Con.) Hall. The . complete list of species is as follows: 1 Spirifer mesastrialis Hall (a) 3 i 2 Tropidoleptus carinatus (Con.) Hall | 3 (r) 3 Camarotoechia eximia Hall ee 5) 2 4 C. stevensi Hall (?) (hase Possibly C. eximia for these two species are very closely related. 5 Goniophora hamiltonensis (Hall) Miller | (et 6 Actinopteria boydi (Con.) Hall (c) 7 Grammysia obsoleta Hall (?) (rr) 8 G. bisulcata (Con.) Hall (rr) 9 Sphenotus solenoides Hall (?) (rr) There are none of the vascular markings on the posterior part of the shell said to be characteristic of this speeies; but in other respects it agrees with it. re. r ae | 7 vy te ae 1 Lg Si ~ « te “ es eee Ewe See NOR gt De ok eee, ; CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 221 - LXXV M. A section was roughly measured from the Schoharie river bridge below North Blenheim along the highway and brook up the steep hill on the eastern side of the river through Mackey’s Corners to the top of Leonard hill in the eastern part of the town- ship. The hill slope is well covered by drift so that the section is not as satisfactory as might be desired. For 440 feet up the hill the rocks are all concealed along the highway, when an ex- posure of bluish shales (M’) occurs in which are a few poorly pre- served fossils. | 1 Liorhynchus multicosta Hall (?) ; (c) The specimens are all quite small and resemble the “ young individual,” fig. 26, pl. 56, Paleontology, v. 4, more closely than any other. 2 Coleolus tenuicinctum Hall (?) (rr) Just the point of apparently a specimen of the above species. : So few fossils were found in these shales that they assist very little in determining their age but judging from the sections on -the western side of the river at North Blenheim it seems probable that they are not older than the Sherburne formation. 40 feet higher are coarse ‘grained, thin gray sandstones (M*) which con- _ tain more fossils both in number of specimens and species, as wiil be seen by following list: 1 Spirifer mucronatus (Con.) Bill. (c) | 2 Chonetes setigera Hall Te ale 3 Tropidoleptus carimatus (Con.) Hall (2) 3 4 Leda dwersa Hall (rr) 5 Orthonota undulata Con. (rr) 6 Schizodus appressus (Con.) Hall (rr) 7 Orbiculoidea sp. (rr) The species in this list are Hamilton and on account of their stratigraphic position they are not diagnostic. The outcrop is probably in the Ithaca formation and is something like 800 feet below the fossiliferous sandstones of LXXV N2, on the hill to the southeast. Then for about 390 feet the rocks are mostly covered till in the upper part of the small brook thick bedded, coarse, 222 NEW YORK STATE MUSEUM ee as grayish sandstone occurs alternating with smooth, greenish shale eho (M4). On the highway just east of the old “state road” at the Brown farm are red and greenish shales (M®) at an elevation of 1020 feet above the river. The difference in altitude,between these shales and the reds at LXXVN!, on the hill to the southwest, is 140 feet, but the stratigraphic difference is much less on account ~ of the southerly dip. These shales which are the first reds seen on this slope of the hill were regarded as marking the base of the Oneonta formation and are so represented on the map. One and one half miles to the northeast are the red shales of XXIX M$ at 1250 feet above the river, and if XXIX M8 and LXXV M3 are in the same horizon then there is a dip of 150 feet a mile to the southwest. At the top of the divide three quarters of a mile west of | Mackey’s Corners are: coarse grained, greenish sandstones asso- ciated with red ones. This locality is approximately 330 feet higher than the first reds at M®, or some 1350 feet above the level of the Schoharie river. The country then descends to the east through Mackey’s Corners to the head of the eastern fork of the Plattenkill or Flat creek at the foot of Leonard’s hill. Plenty of bright red shales occur here (M’) as well as along the highway toward Beam Center. According to the barometric readings these shales are 195 feet above the lowest reds at M® or 1215 feet above the Schoharie river; while from the creek to the top of the hill is 600 feet. This makes the top of Leonard hill at least 1815 feet above the Schoharie river at North Blenheim. The altitude © of the North Blenheim bridge, according to Guyot, being 800 feet A. T. this section makes the top of Leonard hill 2615 feet A. T. The above section is a fairly accurate one for Guyot determined the elevation of Leonard hill by means of the mercurial barometer to be 2649 feet A. T.%, which is only 34 feet more than that for the section just described. The slope of the hill is partly covered, but the exposures of rocks show an alternation of greenish gray, coarse grained sandstones with red shales and sandstones from Amer. jour. science, 3d ser. 19:450. See p. 449 for elevation of North Blenheim. No.7} MSLCTION FROM NV. GLE NHE/M LEONARD'S HILL. eS Sa —— Me 70 TOP _o Tor of LEONARD HILL. COARSE CR EENISH-ERAY SANDSTONE. EO SHALES AND SANDSTONE. FEO SANOSTONE. GREENISH-EAAY SANDSTONE. OWE ONTA. 370 N16| 9&0 SHALE WEAR Foor OF LeowsZ0 HILL. AEO SHALE AT HEAQ OF FLAT CHEER. Ue| Bevisn sawosTrone wiTH FOSSILS. 125 Me fléo srAace BASE of OM EONTA (7) M4| GFAVISH SANOSTONE AND GREENISH SHALE Weed ITHACA THIN GRAY SANOSTONE WITH FOSS/LS. BLUISH SHALES WITH FOSSILS, SHERBURNE : \ VE) Lever or Stn OHARIE CREEK, No.6/,A4. SECTION OD HIML SOUTH OF CUWNLIVILLE AE0 sanosrowe NEAR TOP OF HILL 60| PARTLY cove pED ° MOSTLY FEO SANDSTOWE HED THIN SANDSTONE , TOP CF THIRD POINT ON Mik, WEODISH SANDSTANE , SECOND pornr. CRAY THIN-BE0DEO SAN OSTONE. FURST POINT OF H/LL, PPOMINENT LEDGE OF GREENISH-GARAY focH. BASE OF GRAY LEDGE, PED SANOSTONE WEARLY CONTINUOUS EXPOSURE OF THIN-8EDOED COARSE CA AVIS AF SANOSTGWE. RED SHALE HEO ANO GRay SANOSTINE AND SHALE. FRREOAND GRAY SANOSTONE AND SHALES. GREEWISH-GRAY SANDSTOWE. FREQ ANDOGRAY SAV DOSTONE a ONEONTA Cove wED ALUNG HIGHWAY. Leyec of LL MISS Hitt AT ConESVILLE, BES ‘ABOVE SCHOHAR/E RIVER AT G/LBOA Wo.1b, 2. SECTION SOUTHWEST OF LVN OSTWVILLE WEAR TOP OF HILL OW HEH Way Hoarzon of LOOSE FOSS/LS THIN GLUE SANOSTONE FED SHALE ON OAD Base oF. ONEONTA CovereEo STHACGA ZB, LEVEL oF CarsHritc. CHEEK. ~~ ee et ee ee ee me ie kk ve y Wig Sys Ny ~ 7 Tie aaa ee ; \& Sy =" Seite raged HNOLSANVS VEINOWNO “HITIASHNOD ,,“SMOOYU AHL ,, © QOGYo: vo 10IanaTIVHIGOOMNANE € yal 4 eae | FL old .*; aes er ah, Sy ht SR sd Ee i I Chie At Ase eRe } Bee , y ee r ih, t Paes ey « oS bbe Roan be ae eglacah Aa hae aie a ee | Ra Aye ce TEs Nae ‘ PENA Ya te : . tt Pee eS Se a vd nee ma ae ha * 7% y , : i : Re 5} Sta } 7 ip? 4 ; ata SiGe Broken specimens ; _ 26 Nucula corbuliformis Hall | (rr) 40 feet above the base of zone B* are greenish and bluish argillaceous shales (B®), the interval between the two zones being partly covered. The greenish to olive shales in lithologic appear- ance resemble the shales of the Sherburne formation, but they alternate with bluish, slightly sandy shales which contain oc- casional fossils. One stratum of sandstone four to five inches in thickness contains a large number of clay pebbles. Above this zone the rocks are again concealed for nearly 50 feet when there is another outcrop of bluish to greenish argil- > (eh as laceous shales (B°) by the road side. The bluish shales contain z quite a good many specimens of small Hamilton lamellibranchs as will be seen from the accompanying list. In one thin layer near the base of the zone they are specially common while a little higher is a thin layer of calcareous shell rock in which are numerous specimens of Camarotoechia. The fauna is: 1 Atrypa reticularis (Lin.) Dal. (ec) 2 Spirifer mucronatus (Con.) Bill. ye (rr) CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 243 ao SS: granulosus (Con.) H. & C. (rr) 4 Chonetes setigera Hall (rr) 5 Orthonota undulata Con. (c) 6 Nuculites oblongatus Con. (c) Small specimens. 7 Palaeoneilo constricta (Con.) Hall (rr) 8 Grammysia bisulcata (Con.) Hall (rr) 9 Pterinopecten vertumnus Hall (?) (rr) 15 feet above the base of zone B® and 940 feet above the top of the Onondaga limestone are coarse, bluish, arenaceous shales (B") containing some fossils as follows: 1 Chonetes coronata (Con.) Hall ; rat) _ 2 Spirifer mucronatus (Con.) Bill. (rr) 3 Pterinea flabella (Con.) Hall (r) 4 Actinopteria boydi (Con.) Hall 5 Nueulites oblongatus Con. | 6 Bryozoan : (rr) These are the highest rocks of the section in which Hamilton fossils were found and must be regarded as forming the top of that formation; in fact the greenish shales of B®, 65 feet lower, are transitional from the Hamilton to the Sherburne formation and perhaps might be considered as at its top, but it is thought better to classify the succeeding 65 feet of rocks which contain a fair Hamilton fauna with that formation. The difference in altitude gives a thickness of at least 940 feet for the Marcellus and Hamilton formations in this section; but where observed there is a dip from 14° to 24° a mile to the southwest which would add from 475 to 780 feet, making the thickness of the formation between 1415 and 1720 feet. For about 50 feet above zone B’ the rocks are covered when a heavy ledge of coarse grained sandstone (B®) varying from a slightly greenish gray to bluish gray color and splitting into thin dayers which in places have a somewhat crossbedded structure, - is reached in the field on the western side of the road. A little AA NEW YORK STATE ‘MUSEUM ea higher on the highway and to the east are soft, greenish, argil. ; laceous shales with occasional harder layers. About 25 feet. | above the sandstone is a layer of mottled red and green shale _ ~ : (B™) by the side of the road. This is the first indication of on 7 red rocks and the exposure is within about 50 feet of the top: n> of Bradt hill. The top of the hill on the highway is a little _ north of the four corners and from the mottled shales to this. a point, which is about 55 feet higher, the rocks exposed are all. greenish shales which apparently are in the Sherburne formation. 2S % The top of Bradt hill is 1070 feet higher than the Onondaga lime. stone at West Berne or barometrically some 2040 feet A. T. About three quarters of a mile to the east of Bradt hill and hollow is another high hill called West Mountain near the top of which are coarse Hamilton sandstones, the shaly layers con- taining abundant fossils.. These sandstones varying from eray | to bluish gray in color, form a conspicuous ledge on the western * side of the hill, are rather coarse grained, and on the weathered surface split into thin layers from one half to one inch in ons ie Py ness. : Across Bradt hollow to the northwest of Bradt hill and ~ West mountain in Schoharie co. is Mt Sagerwana or Cotton hill, a conspicuous peak the upper 800 feet of which is in the. -Marcellus and Hamilton formations. XXXVIII At. On the highway leading down into the valley of Stony creek above Huntersland to the southwest of the four cor. | ners on top of Bradt hill are soft, argillaceous and thin arenaceous shales in which Hamilton fossils are quite abundant. The best exposures are three quarters of a mile ENE of Huntersland — and approximately 310 feet lower than the Bradt hill four — corners. The following species were collected: 1 Chonetes coronata (Con.) Hall (aa) 2 Spirifer mucronatus (Con.) Bill. (c) 3d N. audaculus (Con.) Whitt. 3 (r). 4 8, granulosus (Con.) H. & C. (?) (Tigra S 5 Camarotoechia congregata (Con.) H. & C. | (Cc) ; --- -‘GLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 6 Orthonota undulata Con. 7 Modiomorpha concentrica (Con.) Hall 8 Pholadella radiata (Con.) Hall . i 9 Grammysia bisulcata (Con.) Hall 10 Schizodus appressus (Con.) Hall 11 Pterinea flabella (Con.) Hall 12 Orthoceras crotalum Hall - 13 Microdon (Cypricardella) tenuistriatus Hall 245 (c) (rr) (rr) 0) (rr) (rr) (rr) (rr) On the highway just west of the Bradt hill four corners are ‘green shales of the Sherburne formation. The Turner schoolhouse, district no. 20, is at the first four cor- ners, one mile south of the Bradt hill corners and some 60 feet lower, and on the highway not far east of the schoolhouse are red argillaceous shales. The southerly dip, however, has carried the rocks down so that these shales are stratigraphically higher than those on top of Bradt hill. These red shales form a conspicuous zone and were mapped as at the base of the Oneonta formation, which covers the high land beyond the first four corners east of the Turner schoolhouse. This region forms the high divide between the head waters of Stony brook, Tenmile creek and the Switzkill, four miles northwest of Rensselaerville and some 600 feet higher. i On the divide to the west of the four corners are bluish gray thin sandstones differing inappreciably from Hamilton sandstones, while some 30 feet lower at the corners are red shales. The coarser | rocks form terraces that slope rapidly to the southwest. On comparison with the Geologic map of New York it will be seen that the boundary of the Oneonta formation for this region agrees a closely with that outlined on the accompanying map except that er the former it is carried somewhat farther northwest, indicating that the red shales mentioned above were considered as forming its base. _ In fact, Darton said, “In mapping the Oneonta formation. a. in Albany county I have assumed:that its base was at the bottom «ft the lowest red shale member because this was the only dis- us ‘ tinguishing feature that I could use as a guide. Probably this 246 NEW YORK STATE MUSEUM horizon will prove on detailed examination to be somewhat. vari. able, but I believe not with very wide limits.” bone About one mile south of the Turner schoolhouse sal near thes 2 southern line of the township is Berne or Turner hill, the highest | hill in the township and perhaps the highest in the county, being — some 180 feet higher than Bradt hill or 2220 feet A. T. It forms — the high divide between the head waters of Stony creek and the Switzkill on the north and Tenmile creek and other branches of ~ Catskill creek on the south. Red’ shales and sandstones which are in the Oneonta formation outcrop near its summit as well as to the south in the northern part of Rensselaerville township. : In the southern part of Berne township along the principal west- ern branch of the Switzkill are thin blue shales and sandstones, some layers of which are irregular and contain iron concretions. The bluish shales are sparingly fossiliferous, containing very mucronate specimens of Spirifer mucronatus (Con.) Bill., and the recks are in the Hamilton formation. The dip is heavy to the east of south. At the bridge over this branch, one quarter mile ~ above the Switzkill and one and one half miles northwest of South Berne are coarse blue Hamilton shales. LV ©. To the east of South Berne and the Switzkill is a steep hill known as the Agrippa hill, the crest of which is perhaps one —_— and one half miles from, and some 500 feet higher than the Union hotel in that village. The western slope of the hill is well covered’ by drift but on the eastern side there are more frequent exposures. of shales and sandstones. To the east is the head of the Foxkill,. which has not cut so deep a valley as the Switzkill, and a section was constructed from this valley beginning perhaps one and one quarter miles WNW of Reidsville and extending to the top of the - hill. a 13th an. rep’t N. Y. state geologist, p. 240. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 247 SECTION OF THE EASTERN SIDE OF AGRIPPA HILL LV C 275’ ;———, Top of Agrippa hill | Ce mainly covered (ue 198’ |——-— 8’ | ©® Bluish shales with abundant fossils 190’ |——— | C# Bluish gray sandstone: Alexander quarry 15’ : : a 120’ | C3 Partly covered but showing shales alternating | , with sandstones . 55’ j———| C? Bluish sandstone: small quarry ‘C! Bluish fossiliferous shales Q’ = Head of Foxkill The bluish argillaceous shales of C! are exposed along the - highway near the eastern base of the hill and certain layers are very fossiliferous. The species collected are as follows: ,1 Spirifer mucronatus (Con.) Bill. (c) 2: SS. granulosus (Con.) H. & C. (?) (rr) 3 Camarotoechia sappho (Hall) H. & C. (a) 40. congregata (Con.) H. & C. (Cc) 5 Tropidoleptus carinatus (Con.) Hall (rr) 6 Chonetes scitula Hall . (r) (6 5 ies setigera Hall . (c) 8 Goniophora carinata (Con.) Hall (rr) _ 9 Pterinea flabella (Con.) Hall — | (rr) of the hill is the extensive flagging stone quarry known as tl Alexander or Agrippa. The lower part of it (C‘) consists of 1 . stone are three feet of blue ee which is not used. Th NEW YORK STATE Bp MUSEUM oa *, F Above the chates of Ct the slope is case covered, bu are occasional ledges of thin bedded, bluish sandstone alte with shales. Small quarries have been opened in some of t ese ledges, the stone splitting into six inch layers. Toward the t feet of bluish gray sandstone which is worked for flagging, si and gels Near the middle: is a layer — for use, 1 = by the quarrymen. Again at the aoe of the even bedded aa of bluish, argillaceous shales (C°) which weather to an iron So and contain an abundant Hamilton fauna, specially Lamelli- 2 branchs. The following species were collected in these BeehES , 1 Spirifer audaculus (Con.) Whitfield S. mucronatus (Con.) Bill. . S. granulosus (Con.) H. & C. a Boe Productella dumosa Hall . ay Tropidoleptus carinatus (Con.) Hall mo é Dignomia_ alveata Hall ; | Camarotoechia congregata (Con.) H. & C. Ce sappho (Hall) H. & C. ‘Glyptodesma erectum (Con.) Hall CoN FS 1K & Grammysia circularis Hall G. bisulcata (Con.) Hall Tellinopsis subemarginata (Con.) Hall ftp pet fet wore oS LInorhynchus multicosta Hall pas iw Modiomorpha concentrica (Con.) Hall pond Ot Gontophora hanultonensis (Hall) Miller jt =r) Nyassa arguta Hall Macrodon hamiltoniae Hall -Modiomorpha subalata (Con.) Hall Nucula corbuliformis Hall bP He owvan Nuculites triqueter Con. - QLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 249 21 Palaconeilo plana Hall : (c) 22° P. perplana (Con.) Hall (r) _. 23 Pterinea flabella (Con.) Hall | (rr) 24 Pterinopecten vertumnus Hall (r) 25 Loxonema hamiltoniae Hall (?) (rr) 26 Tentaculites attenuatus Hall (?) (rr) 27 Strophalosia truncata (Hall) Beecher (c) 28 Liopteria bigsbyi Hall | : (c) 29 Aviculopecten princeps (Con.) Hall (?) (c) 30° Orthoceras crotalum Hall (r) ol O. constrictum Van. (rr) The above fauna shows that the quarry is in the Hamilton: formation and it appears probable that it continues to the top of Agrippa hill which is only about 77 feet higher. LV Bt. In the southeastern part of Berne township near the head of Hannecrois creek is the little hamlet of Reidsville. In the vicinity of this village are several flagstone quarries from which large quantities of stone have been shipped. Just to the east of Reidsville is the Cumming’s quarry which has the follow- ing section: pee = Soil 33 | Thin bedded blue Hamilton sandstone (“ callous” layer of the Peay) 24’ | Blue flagging sandstone which splits into layers on the average about 24 inches in thickness ———| Bottom of quarry The dip in this quarry is about 3°S10°W 250 - NEW YORK STATE MUSEUM LV B’. A few rods to the east of the Cumming’s quarry isthe __ Blue stone company quarry which in the lower part has five feeny - cight inches of flagging stone called “blue stone ” by the quarry: men. The flags split into layers varying from two and @ half to. three inches in thickness, while the layers from four to five inches ae s s in thickness are used for curbing. At the top of this flagging Pea stone is a layer which thins rapidly toward the northern end of the quarry. In the southern part it is one foot, seven inches in Bie thickness, while 100 feet farther north it has decreased to three _ inches. Above this are 7 feet of thin bedded sandstone, thrown away in quarrying, that contains Spirifer mucronatus (Con.) Bill. and plant stems. Fossils however do not occur abundantly. The section is as follows: 122’ |———, Soil 7’ | Thin bedded sandstone : Stripping of the quarry 52’ |——— Layer of varying thickness 52’ | Bluish gray sandstone Quarry stone ———| Bottom of quarry There ig little soil on the rock so that the stripping is confined to the seven feet of thin sandstone layers. The following deter- minations of dip were made: About 3° S10°W 2° to 24°W 4° SW It varies however in different parts of the quarry since the > lower layers in the northern part are nearly level. One line of joint runs S10°W and N10°E, and this is crossed by another set trending east and west. From the above description it will be seen that the greater part of Berne is covered by the Hamilton and Marcellus formations, _ CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 251 the exceptions being in the northwestern and northeastern parts. where the Onondaga limestone occurs, and in the southwestern where the Sherburne and Oneonta formations are found. The line between the Hamilton and Sherburne formations enters the township from Schoharie co. on the hillside to the south of Stony creek which it follows to near its head when it turns to. the north and circles around the upper part of Bradt hill and then runs southeasterly into the northeastern part of Rensselaer- ville township. The lowest heavy line of the reds which is called: the base of the Oneonta formation follows a nearly parallel course though somewhat farther to the south and west than the Hamilton-Sherburne line. Rensselaerville Rensselaerville lies to the south of the western half of Berne,. forming the southwestern township of Albany co. It is: bounded on the east by Westerlo township, on the south by Greene co. and on the west by Schoharie. Its surface is mostly high land forming either a part of the Helderberg plateau or the northeastern Catskills. Its principal streams are the : Catskill creek which flows across the southwestern part receiv- 3 ing the Potter hollow branch from the west, both streams flanked by high and steep hills, and Tenmile creek which flows in a southerly direction across the eastern part of the township re- ceiving Eightmile creek from the east at Meduea, and enters the Catskill creek below Oakhill in Greene co. About one mile west of Tenmile creek is a brook which flows parallel to it across. . the southern half of the township, entering the Catskill creek at Oakhill, which may be called the Oakhill brook. ae striking characteristic of many of the hills in this and other townships of the Helderberg region is the steep northern slope. and the gradual descent to the south due to the strong dip in that general direction. An excellent illustration is afforded by the ridge to the east of Rensselaerville which ends very abruptly on the north and slopes gradually to the south.. The steep northern end of this hill is clearly defined from the top of Agrippa P9252 3 _ NEW YORK STATE MUSEUM 2 Ae hill to the east of South Berne. The rocks in the high land of the northwestern part of the township are well covered ‘by soil’ and drift and there are two small glacial lakes in the north-. western corner. Near the head of the brook which enters the Catskill at Preston Hollow, about two and one half miles west of — Rensselaerville, are red shales which are approximately 950 feet higher than those on the bank of the Catskill below Preston Hollow. LVI A‘. On the bank of the Preston Hollow brook, approxi- mately 160 feet higher than the red shales on the Catskill is an olive shale at the base, then a crumbly, irregular shale, capped by @ coarse sandstone four feet thick (A’). Near the southern end of = this cliff there is a break in the rocks with a small overthrust fault. At this place the crumbly shale is shown near the top of the cliff, while at its northern end it is not more than three feet above the water. Gn the western bank of Catskill creek three fourths of a mile below Preston Hollow, and just above the bridge on the Presten Hollow-Cooksburg highway, is a fine exposure of red, argillaceous shale 20 feet thick (A‘). Near the center of the ledge is an olive band while some of it is mottled red and green. At the southern end of the cliff is a stratum of coarse grained, grayish sandstone which has either fallen or been pushed up. There is a small anticline shown in the cliff so that it is not possible to make any general estimate of the dip at this locality. These red rocks are near the base of the Oneonta for- mation which extends only about one mile farther south along the creek valley. This bluff of red shale is barometrically 950 feet lower than the red shale near the head of the Preston Hollow brook, 1350 feet lower than the top of Berne hill and 1100 feet lower than the base of the red shale near the Turner schoolhouse in the southwestern part of Berne township. The distance between these two localities is nine miles which gives a SSW dip of approximately 120 feet a mile. The Oneonta formation extends up the Catskill valley from south of Cooksburg to near the county line below Living- - | No. 50, 6. SLC71UN OF HILL14 M1. NORTHEAST OF JLNISEL MULL E TOP OF A/LL Biocny geo snares ONEONTA ith BLOCH VY CGHEEN SHALES BLVISH SANDSTONE Mainty covezeo SHE ABUANE SHALES WITH HAMILTON FoSssILs 6-8 of rr aceine-stove HAMILTON — 4YO'ABOVE RENSSELAERVILLE HOTEL. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 253: stonville where lower rocks occur. Again below Cooksburg in the northern part of Durham township, Greene co. for a few - miles the creek has cut through the Oneonta formation and shows. along its valley the rocks of the underlying Sherburne formation. XXX C. The ridge to the east of Rensselaerville ends in an ab- rupt slope facing the valley of the Switzkill about one and one third miles directly northeast of ‘the village. At the base of the hill is a small quarry showing some six to eight feet of blue flag- ging stone covered by blue argillaceous shales in which Hamilton fossils are common. ‘These shales in lithologic characters are” very similar to the typical Hamilton and the exposure is in this. formation though near its top. The following species were collected and it will be seen that the fauna is very similar to that of the shales in the Agrippa quarry (55C®) near the top of Agrippa hill. Itis probable that both exposures are in the same general zone of the Hamilton formation: 1 Productella dumosa Hall | (a) 2 Spirifer mucronatus (Con.) Bill. : Ree oC; oS. granulosus (Con.) H. & C. (c) 4 8. audaculus (Con.) Whitfield : ; (rr). 5 Tropidoleptus carinatus (Con.) Hall (c) 6 Camarotoechia prolifica (Hall) H. & C. (1) 7 Chonetes mucronata Hall ; (rr) 8 Orthothetes chemungensis (Con.) H. & C. var. arctostriata Hall .- (rr) 9 Nyassa arguta Hall (r). 10 Nucula corbuliformis Hall | (a) 11 Tellinopsis subemarginata (Con.) Hall (r) 12 Palaeoneilo perplana Hall (rr) 13 Sphenotus solenoides Hall | (rr) 14 Grammysia alveata (Con.) Hall (rr) 15: G. circularis Hall ; (r) 16 Paracyclas tenuis Hall (?) oa, (rr) 17 Glyptodesma erectum (Con.) Hall | (c) 18 Aviculopecten fasciculatus Hall (?) AS (a) 19 Pterinea flabella (Con.) Hall hea (r) so 3): ame NUW YORK STATE MUSEUM 20 Actinopteria boydi (Con.) Hall . eae 21 Liopteria sp. — 22 Pleurotomaria sulcomarginata Con. 3 Gs 23 Bellerophon thalia Hall (?) Oo bey 24 Orthoceras crotalum Hall ies e cn 25 Phacops rana (Green) Hall | (rr) : 26 Crinoid calyx". - ae (rr) e Above the quarry the rocks are well covered, but about 215 | feet higher than its base is a ledge of bluish sandstone on top’ of which are green blocky shales (C*). Near the farm house at the northern end of the hill about 285 feet above the Hamilton fauna are blocky red shales (C*) which show along the crest of the ridge at various places, following it to the south,and specially well on the Rensselaerville-Clarksville highway, crossing it about one mile farther south. At the four corners one and one quarter miles east of Rensselaerville is a good exposure of the red shale. To the east at the highest point on the road is red shale again and the terrace on the northern side of the road shows its rise to the north very nicely. Along the road down > the eastern side of the ridge are first green shales below the reds of the terrace, then reds again showing a thickness of more than 60 feet of the Oneonta formation in the upper part of the ridge. On the road 160 feet lower than the crest of the ridge ~ are greenish and bluish sandstones which are probably near the same stratigraphic position as the zone of XXX C at the northern end of the hill. The red shales of this ridge were noted and referred to the Oneonta formation by Darton who stated that in Albany co. “From the northeastward the first exposures of the Oneonta formation are near the summit of the high ridge ~ east of Rensselaerville, where the red shales outcrop along the road and in the adjacent fields over a narrow belt. This belt widens to the southward and covers all of the high region along the Westerlo-Rensselaerville boundary.’ XXXE. To the northeast of section XX XC and about two miles northeast of Rensselaerville is an excellent quarry known as the a@13th annual report N. Y. state geologist, p. 239. ANOLSOWVIA NOLTINVA ‘ATIIAUAVIESSNGAY AO HLYON AYUYVNO LYUVMALS CT 981d CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 255 Stewart flagstone quarry from which a large-amount of flagging has been shipped. There is from four and a half to six feet of good flagging stone that splits into layers, three, four and eight inches in thickness covered by 11 feet of stripping composed of shale and soil. The blue argillaceous shales on top of the flag- ging stone contain an abundant Hamilton fauna and the rocks belong in the upper part of that formation. The following species were collected: 1 Spirifer granulosus (Con.) H. & C. (c) 2. mucronatus (Con.) Bill. (r) 3 Tropidoleptus carinatus (Con.) Hall | (c) 4 Camarotoechia prolifica (Hall) H. & C. (rr) 5 Orthis (Rhipidomella) vanuxemi Hall (2) | (rr) Internal impression poorly preserved. 6 Orthothetes chemungensis (Con.) H. & C. var. arctostriata Hall (rr) Tt Productella dumosa Hall (r) 8 (2?) Orbiculoidea sp. (r) 9 Orthonota (?) parvula Hall (rr) 10 Nucula corbuliformis Hall (c) BLN. Varicosa Hall | (er) 12 Palaeoneilo perplana Hall (rr) 13 Grammysia circularis Hall (r) 14 G. lirata Hall (rr) 15 Modiomorpha subalata (Con.) Hall (?) (rr) 16 Goniophora hamiltonensis (Hall) Miller : (rr) 17 Glyptodesma erectum (Con.) Hall . (r) 18 Aviculopecten fasciculatus Hall (?) (c) 19 Actinopteria boydi (Con.) Hall - (rr) 20 Bellerophon brevilineatus Con. (rr) 21 B. — thalia Hall (rr) This quarry is nearly two and a half miles southwest of the Agrippa quarry on the hill east of South Berne and the dip is about 14° S 35° EK. The accompanying picture serves as a fair illustration of the flagstone quarries in the upper Hamilton of Albany county and gives a clear idea of the one just described. t 256 NEW YORK STATE MUSEUM XX AL Tenmile creek flows Heonen the western ae of Rensselaerville village forming a glen of some depth. In the lower part of the glen about opposite the village hotel are ledges of shales and sandstones. Part of the shales are of an olive color 3 and argillaceous, splitting into very small pieces while others are more blocky in texture and mottled blue and greenish in — te color. The sandstones contain numerous irregular, fucoidal-like markings on the surface of the different layers. Again the surface of some of the layers is irregular as though deposited in | Shallow water where they were affected by currents and waves. The appearance of these rocks is similar to that of the transi- tional Hamilton in the North Blenheim region of the Schoharie valley. No fossils were found. XXX A”. Above the lower falls and bridge and extending to the © foot of the principal fall 40 feet above the base of the section — - which is only a short distance west of the village, are bluish shales, some of the layers forming a fairly hard sandstone in which fossils are common. The smooth shales alternating with these coarser layers contain very few, if any, fossils. The fol- lowing species were obtained from the sandy layers of this zone: 1 Camarotoechia prolifica (Hall) H. & C. (Gc) 2 Spirifer granulosus (Con.) H. & ce Qe oS. mucronatus (Con.) Bill. : (rr) 4 Chonetes setigera Hall (Eyes 5 Strophalosia truncata (Hall) Beecher (2) pe (r): - 6 Goniophora hamiltonensis (Hall) Miller ; (r) 7 Grammysia magna Hall (rr) 8 Palaeoneilo constricta (Con.) Hall ~(r) 9 Orthonota undulata Con. (rr). ~ 10 Nyassa arguta Hall . (ery: 11 (?) Sphenotus truncatus (Con.) Hall ~ | (rr) Quite imperfect specimens. : 12 Pterinea flabella (Con.) Hall Sate 13 Actinopteria boydi (Con.) Hall | Regn 14 Loxonema hamiltoniae Hall (TERY Ss 15 Tentaculites attenuatus Hall (PI), 16 Taeniopora exigua Nicholson , | (c} N0.50, A. SECTION COGAN Ay HENMELALMULLE LEVEL OF Wrosorus LAME ! PED AND GREEN SHALES yi at } BLUYISH SANOSTOME FFE QOIS 4 -GAAY MASSIVE SANOS TONE HEO AND GREEN SHALES SLOCHY FEO Sy ZL ES. BASE gf QNEONTA SOME WOTTLEOD BRED ang GREEW SYALES [itn NNN BLU/$H ANDO GHEE W SHALES SHERBURNE FOOT OF YVepEG FALLS 3 BLUISY SHALES WITH FOSS/LS, OLIVE 4NO0 SLUISH SH AL Fs 4NO SAND ST 0 NO FOSSILS. Hl hoa (Ny at (jl il! 1) {qll! (iyi | No. 50, ILC 710 N Bee OLIN 2.5 MIS. OF REWSSELAERVILLE 53 AED SANOSTONE ATBRINK OF FALLS COAASE FED SHALE UPPER PAAT OF FALLS BASE of ONEONTA 2S Be Bee 22 4G) ==. == : | ee GREEN SHALE —s =—- —=- = Foor OF FALLS. BLVE AAGILLACEOUS SHALE wiT# LAM ELL/BRANCHS. Go SHE REUANE PLUISH AND GREN/SH AAGILLACE OUS SHALES, PLANT STEMS. COVERED BHIOGCE WER CREEL, 250' BELOW RENSSELAERVILLE Ho TiER [os oat CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 257 The above is a Hamilton fauna and apparently these shales are at the top of that formation as shown by the higher rocks. Succeeding the fossiliferous shales at the foot of the falls are i bluish and greenish shales (A%) with some mottled red and green shale in the upper part. At an elevation of 70 feet above the foot of the fall is a stratum of red, blocky shale (A*) succeeding which are 25 feet of alternating red and green shales extending up to a massive sandstone which forms the brink of the upper falls. The ved shale at the base of this zone was taken for the base of the Oneonta formation and is so represented on the accompanying map. If it represents the same zone as XXX°C® at the northern end of the ridge 1.7 miles to the northeast then the dip to the sw is ~ 153 feet a mile. At the top of the falls is a massive reddish gray sandstone (A°) 10:feet or more in thickness, the top of which is 145 feet above the base of the section. On this massive sandstone are thinner bluish sandstones. In the wall of the dam is a large block in which are the following species: 1 Spirifer granulosus (Con.) H. & C. (?) che nee 2 8: mucronatus (Con.) Hall (cr) 3 Chonetes coronata (Con.) Hall | (rr) 4 Camarotoechia prolifica (Hall) H. & C. (rr) 5 Orthis (Rhipidomella) vanuzemi Hall (rr) Farther up the creek are reddish, greenish and mottled shales (A°) which extend to the dam at the lower end of Myosotus lake 200 feet above the base of the section. The above section is” shown in tabular form in the reproduced diagram. XXX B’.Two and eight tenths miles to the sse of Rensselaerville is a gorge known as Felter’s glen which has been cut by an eastern branch of Tenmile creek. The lowest rocks (B?) which are green - argillaceous shales occur about 80 feet higher than the highway bridge. Above these occur layers of bluish sandstone with a slightly reddish tint, which contain sand holes and plant stems. These rocks are referred to the Sherburne formation oh account of their stratigraphical position, lithological appearance and the 258 NEW YORK STATE MUSEUM absence of fossils. Some 60 feet higher than the lowest shales _ at the foot of Felter’s falls is a layer of blue, argillaceous shale a s (B*) in which Estheria sp. are common. Dr John M. Clarke after examining them says “I know no other species in our Devonian except my EL. pulex, which is a little fellow.” (Letter, dated Mar. 21, 1898) \ Immediately above the blue shales are smooth, green shales breaking into irregularly shaped pieces in which no fossils were | found. The green shales are about 40 feet thick, but in the upper oe part of the falls and the rocky sides of the glen are coarse, blocky, {tips Se Mt red and mottled shales (B+). This zone is five feet thick and part | of it is very arenaceous almost forming a sandstone. This ae stratum is the lowest of the clearly red rock seen in the glen . vie and is called the base of the Oneonta formation. If the lowest iy cs red shale (XXX A*) in the Rensselaerville glen is at approximately — ie : the same stratigraphical position then there is a dip to the sse of 62 feet a mile. It appears probable that the red shale of XXXC® at the northern end of the ridge 3.7 miles north of Felter’s glen — represents about the same zone as B! in this glen which gives a , é dip directly south of 117 feet a mile. Directly on the top of the zone of red shale and 185 feet higher than the base of the section is a red sandstone (B°) which forms — the brink of Felter’s falls. Above the falls for a short distance are greenish, irregular shales, then red and mottled red and green argillaceous shales, but after a few rods the rise is very gradual and the rocks are concealed by drift. The red shales are shown ai various places along the ridge to the north of Felter’s glen toward the Rensselaerville-Clarksville highway and also on the sides of the hills flanking Tenmile creek to the south of the glen. On the western side of Tenmile creek on the highway a short distance north of Medusa and five miles south of Rensselaer- ville are red argillaceous shales 125 feet above the bed of the creek in the village, while on the same road just north of Medusa are mottled red and green shales only 45 feet above the creek level. In the creek bed from the highway bridge to the foot of the dam are greenish and bluish shales and sandstones appa ae ~ . te: Fs } e vt = a _ Catskill creek valley. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 259 in the upper part of the Sherburne formation. This upper part of the Sherburne formation is shown at various places along the lower valley of Tenmile creek to its junction with the Catskill in the northern part of Greene co. and for some distance along the valley of the latter creek both below and above the mouth of Tenmile creek. The lower line of the Oneonta formation along these two creeks is quite accurately shown on the Geologic map of New York except that it is carried several miles too far down the Westerlo To the east of Rensselaerville and south of the eastern half of Berne township is Westerlo which occupies a central position in the southern tier of townships in Albany co. The principal | streams are Basic creek which rises in the northern part and flows southerly across the central part of the township, Hight ~ Mile creek which rises in the western part and flows southwesterly into Tenmile creek and Hannecrois creek which flows across the northeastern portion of the township. The general elevation is less than that of Rensselaerville or Berne townships and the vari- ous ridges extending in a general north and south direction are not as steep. The western half of the township is quite heavily covered with drift so that any considerable exposures of the underlying rocks are infrequent. XXX D1. On the western side and near the top of the low hill about one half mile westof Dormansville is oneof the Dormansville flagstone quarries. At the base are three and a half feet of bluish flags on a weathered surface turning slightly reddish, the shaly partings of which contain fossils. Above are eight feet of bluish, argillaceous, somewhat blocky shales which are quite barren of fossils, next, a stratum of sandstone one and a half feet in thickness covered by another stratum of somewhat blocky, argillaceous shales in which small Hamilton lamellibranchs are abundant. These rocks have the lithological appearance of the Hamilton and contain its fauna and are clearly in this forma- tion. The following species were collected: NEW YORK STATE MUSEUM | 1 Spirifer mucronatus (Con.) Bill. Sere re a 2 Tropidoleptus carinatus (Con.) Hall | ey ee 3 Chonetes coronata (Con.) Hall Rie, Hen: ¥ AO, setigera Hall fee: 5 Camarotoechia sappho (Hall) H. & C. eye. Gi tine prolifica (Hall) H. & ©. (rr) (Gree congregata (Con.) H. & C. eae 8 Leda diversa Hall (rr). . 9 Goniophora rugosa (Con.) Miller (Gry 10 Nuculites oblongatus Con. i EE) eg 11 Sphenotus truncatus (Con.) Hall (?) is Were ae Imperfectly preserved. Somewhat resembles Nyassa recta = = Hall. eee 12 Nucula bellistriata (Con.) Hall (a) voy The specimens are smailer than the figures of this species ae ; and are apparently the young, or perhaps the variety hes . noted in the Ithaca at Oneonta. . 4 ' 13 Nyassa subalata Hall (?) Ate 2 XXX D*. Just over the hill mentioned above on its eastern side is a larger quarry, nearly 10 feet of flagging stone showing in its — . Pe lowest part. The sandstone is the same stratum as the flagstone — of the other quarry and the quarry is much better not only on = 3 account of the greater thickness of the rock but also because there is very little shale on top of the flags and consequently less" stripping. A thin sandstone in the shales near the quarry con- 3 tains immense numbers of very mucronate specimens of Spirifer | - mucronatus (Con.) Bill. associated with Chonetes coronata (Congo Hall. The complete list is: | eee 1 Spirifer mucronatus (Con.) Bill. (a) 2S: sceulptilis Hall , Toe (r) 3 Chonetes coronata (Con.) Hall i | (a) 4 Tropidoleptus carinatus (Con.) Hall (a) 5 Camarotoechia congregata (Con.) H. & C. (c) 6 Sphenotus truncatus (Con.) Hall (rr) 7 Glyptodesma erectum (Con.) Hall A 8 Bellerophon patulus Hall (?) + Ty Imperfectly preserved. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 261 _ In places the rock shows a dip of between 2° and 24° S about 40° W. The Dormansville quarries were mentioned by Darton who states that they “are in a bed about 10 feet thick which yielded a very large amount of excellent flagging.”* Darton divided the Hamilton of Albany co. into two divisions, the lower one 600 feet in thickness, which he called the “ Hamilton black shales ” aud the upper one the “ Hamilton flags and shales” 700 feet in thickness. He considered that “The beds of flags are not at any definite horizon, though the greater amount of flag which has ‘been worked is from beds about 250 feet above the base of the series [his upper division]. . . The lower portion of the forma- tion is sparingly fossiliferous, particularly some of the softer thinner flags, which yield a Hamilton group fauna. The upper beds of the series may extend above the limits of the Hamilton group of western New York, but I have at present no definite evidence on this point.’’@ It seems that all of the important flagstone quarries of Albany county are in the Hamilton formation, as stated above, but it will be shown that farther south in Greene and Ulster counties many of the large quarries are above the Hamilton and in the Sher- burne formation. Again the writer considers that in Albany county the upper portion of Darton’s “ Hamilton flags and shales ” are above the top of the Hamilton as he thought they might be and in the Sherburne formation. On the hill east of Basic creek and some three miles northeast of South Westerlo is a prominent ledge (X XX D*) of massive red sandstone five feet in thickness. The surface is very irregular as though it had been worn by the ice. In the field to the east of the highway is a ledge some 15 feet in thickness. At the base is apparently a stratum of fed sandstone, then there are bluish gray sandstones which are capped by red somewhat irregularly bedded sandstones. In the southeastern part of the township about three miles east of South Westerlo are coarse, arenaceous shales and @ 13th annual report N. Y. state geologist, p. 241. 262 NEW. YORK ’ eae Ace MUSEUM thin blue datittenee (XXX D) which ag the lithologie charactente : re of the Hamilton. In places they contain the characteristic fauna of . the coarse Hamilton deposits as Spirifer granulosus (Con.) H. & C., Spirifer mucronatus (Con.) Bill., Chonetes coronata jon) Hall, ete. wp 3 RR the complete list being: | ta 1 Chonetes coronata (Con.) Hall — ae ayers 2 Tropidoleptus carinatus (Con.) Hall (ce) , fi 3 Spirifer mucronatus (Con.) Bill. ; Be. : | 3 R48: sculptilis Hall (rr) 5S. granulosus (Con.) H. & C. (rr) ~ eee 6 Camarotoechia prolifica (Hall) H. & C. (ey Fons CC: sappho (Hall) H. & C. | COURT Rete 8 Orthothetes chemungensis (Con.) H. & C. . § c var. arctostriata Hall 1 eae 9 Glyptodesma erectum (Con.) Hall | (c) 10 Nucula bellistriata (Con.) Hall | (er) 11 Nyassa subalata Hall ~ . (r) 12 Platyceras bucculentum Hall (?) (rr) The rocks of this locality are undoubtedly in the Hamilton formation. Near the highway corners one mile to the west of the Hamilton rocks is red sandstone of the Oneonta formation ~ while below are greenish shales and sandstones, in which no fossils were found, that are probably in the Sherburne formation. The red sandstone is 150 feet higher than the Hamilton exposure to the east and supposing the dip to be 100 feet a mile to the west which is apparently all that it is, then the red sandstone is approximately 250 feet stratigraphically above the Hamilton. On top of the hill one half mile east of South Westerlo is a prominent ledge of greenish red sandstone (XXX D*°) five feet in thickness which on the weathered surface has a dark red color. ae Above is a ledge of clear blue, thin sandstone which is cross- bedded. On the Geologic map of New York the exposures of red rock just described are mapped as in the Hamilton formation which is represented as covering all of the country to the east of Basic creek, its top occurring on the hills considerably west of the creek and South Westerlo. Along Basic creek above and AS “S68 ea Se a he Lo ee Oo ee Oe Sa Ul be whats PO aA i 2 posh! \.e ~ ’? eee eee | x > sp - oP) ea Dit hs Lenn r: Ras eas an bt id nl ee “y, SRC 4 Foire 47 falc, Pa ¥ Vh) wir sg igre ‘ £4 2 f wh ue a+ ~ ‘ vie wl . / we + . Hy ee ‘ 7 ,) ee MWe emg ON ae a esta . nue DN a in (a) ) CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 263 below the bridge at South Westerlo are ledges of rather greenish sandstone and some shales in which no fossils were found. These rocks are 100 feet or more below the red sandstone on top of the ridge east of the creek and are in the Sherburne formation which extends down the creek into the northern part of Greenville township in Greene co. | The exposures in Westerlo and Rensselaerville townships show that red and gray rocks in lithological characters identical with the typical Oneonta formation have replaced the Ithaca formation, and that the reds appear at lower and lower stratigraphic horizons as, the strike of the formations is followed southeasterly from Schoharie co. The line of division between the Hamilton and Sherburne forma- _ tions enters Rensselaerville from Berne township about north of _Rensselaerville village, runs southerly into the Switzkill valley, then about easterly around the northern end of the ridge to the east of Rensselaerville village and then in a general southeasterly direction across Westerlo township. The line is somewhat to the west of Westerlo (Chesterville) and Dormansville and leaves the _ township near its southeastern corner, three miles east of South Westerlo. The drift conceals the older rocks so thoroughly over a large part of Westerlo that it is difficult to trace the line of separation between the different formations. The red shale and sandstone at the base of the Oneonta formation is a much more irregular line than the one between the Hamilton and Sherburne formations. ‘The red shale enters Rensselaerville township near the middle of its northern line to the west of the Switzkill, shows in the gorge of Tenmile creek west of Rensselaerville village and then runs about southerly on the eastern side of the hill to the west of this creek to its end east of Oak Hill in the northern part of Durham township Greene co. Then it extends up the valley of the Catskill across the line into Rensselaerville town- | ship below Cooksburg where it crosses the creek and follows the western side to below Eagle bridge more than one mile below Oakhill, then it crosses the Catskill back to the east and fol- lows the western side of the ridge east of Tenmile creek to its ” ‘ Pass vat . Sa i 264 NEW YORK STATE MUSEUM : northern end northeast of Rensselaerville village. From the ey northern end of the above ridge the direction is in general south- easterly across the southwestern portion of Westerlo in the valley of Basic creek, which it crosses below South Westerlo, in the © northern part of Greenville, Greene co. and runs northeasterly along the ridge east of the creek and South Westerlo till it turns southeasterly again and crosses the line into Greenville about two miles east of South Westerlo. It will be noticed on referring to the accompanying geological map that in the southern part of | Albany and northern part of Greene counties the boundaries of — the formations make frequent loops to the north,. and this is caused by the abrupt northern ends of the ridges between the streams which have a generally southerly direction, so that a line follows down the flank of a hill on the western side of a stream till it crosses it when it follows the rise of the ridge on the east. frequently till it makes the turn around its northern end. As already stated the red rocks of the Oneonta formation extend con- siderably farther east along the southern line of Westerlo than is represented on the Geologic map of New York since they cross. Basic creek to the east below South Westerlo and run southeast- erly across the northeastern part of Greenville township instead of keeping to the west of Basic creek until several miles below West Greenville. . GREENE COUNTY Greene co. lies to the south of Albany and the eastern part of Schoharie co. and extends eastward from Delaware co. 1o the Hudson river., The Schoharie river rises in the Catskills, which cover the western half of the county, and flows in a north- westerly direction till it enters Schoharie co. The eastern face of the high land or plateau out of which the Catskill moun- tains have been carved by denudation ends abruptly, and when seen from the comparatively low land between -the mountains and the Hudson river has the appearance of a high and massive mountain range. To the east of the mountains is a rolling country with low and generally rounded hills till the limestone ridges are tae’ ¥ — . 4 a a CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 265 reached to the west of the immediate valley of the Hudson river when we find folded rocks forming steep hills of considerable ele- vation, composed of the formation belonging in the upper Silurian system and the lower Devonian which extend across the county with a ssw trend about parallel to the course of the river. ‘The principal streams to the east of the Cats- kill mountains are the Catskill creek from the northwest and the Kaaterskill from the southwest which unite just after cutting through the sharply folded limestone hilly west of Catskill and enter the Hudson river near that town. The rolling country to the west between these hills and the base of the mountains is composed mainly of the Hamilton, Sherburne and lower part of the Oneonta formations, while from the upper part of the eastern — border range of the Catskill mountains westward across the county into Delaware and southward across Ulster co. the rocks belong - in the Catskill formation. Northern townships The northern tier of townships in Greene to the south of Albany co. is composed from east to west of New Baltimore, Green- ville and Durham. The great amount of drift found in New Balti- more and Greenville townships similar to that already mentioned in reference to Westerlo rendered it extremely difficult to trace the top of the Hamilton formation. Only a few exposures yielding Hamilton fossils were found in New Baltimore township but this was due in part to the fact that the country examined somewhat carefully was found to be underlaid by rocks near the top of that formation and above it in the Sherburne. By the side of the road in the hamlet of Medway are bluish shales containing a few Hamil- ton fossils, and the rocks are clearly in that formation. The species collected are: 1 Camarotoechia prolifica (Hall) H. & C. (c) 2 Nucula corbuliformis Hall (?) (rr) Broken and poorly preserved specimens. 3 Tentaculites sp. (er) 4 Crinoid segments (c) 266 NEW YORK STATE MUSEUM One and one fourth miles northwest of Medway is the Medway 3 Park hotel and by the side of the small pond to the north of it are fine, bluish argillaceous shales which contain a few Hamilton fossils and are evidently in that formation. The listisasfollows: 1 Chonetes coronata (Con.) Hall (c}) - ‘ QC. setigera Hall | (a) 3 Spirifer mucronatus (Con.) Bill. (c) 4 Camarotoechia prolifica (Hall) H.&C. ea Cc) 5 Nuculites oblongatus Con. | (rr). 6 Tentaculites sp. | | (cr) Imperfectly preserved. : s On the northern road from Medway Park hotel to Grapeville near the top of the ridge between the two branches of Cabin river are fossiliferous rocks which are also apparently in the Hamilton as will be seen by the following species: 1 Spiifer mucronatus (Con.) Bill. | (c)- 2 Chonetes coronata (Con.) Hall : 3 Camarotoechia prolifica (Hall) H. & C. (r) 4 Orthonota (?) parvula Hall eh meh 50: ' carinata Con. jy (rr) The top of the same ridge however on the southern road one half mile farther south is composed of rather greenish, unfossil- iferous shales similar in lithologic appearance to the Sherburne. On the highway to the east of Cabin river one mile below Grape- ville and 150 feet lower than the greenish shales on top of the ridge to the northeast are bluish shales containing Hamilton fossils. Passing westward these were the last Hamilton fossils seen and the top of the Hamilton has been represented as cross- ing from Westerlo the northeast corner of Greenville into New Baltimore township. Then it runs along the western side of Cabin river as far perhaps as one mile below Grapeville, when it crosses the river, makes a loop round the ridge on the eastern side and follows that southeasterly toward Urlton (formerly Jacksonville) in Coxsackie township. There are possibly reddish rocks on the ridge west of Grapeville, but one and one half miles farther west on the ridge east of East Greenville are clear red CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 267 argillaceous shales. A mile east of the village is a good exposure of the red shales and along the highway from East Greenville to Greenville are several outcrops of red shale and sandstone. At the top of the hill just east of Greenville are thin red sandstones. The base of the Oneonta formation is represented on the map as crossing the northeastern part of Greenville township to the east of East Greenville and the southwestern corner of New Balti- more into the northwestern corner of Coxsackie township. This line of the base of the reds or Oneonta formation is represented on the Geologic map of New York as on the ridge west of the creek at West Greenville, while as a matter of fact it is on the Norton hill—East Greenville highway four and one third miles farther east. LVII D2. From East Greenville across the northern part of Greenville and Durham townships the rocks all belong in the One- onta formation till the valley of Tenmile creek is reached east of Oakhill in Durham. Not much above the creek’s mouth by the highway and opposite the mill on its western bank are fine blue argillaceous shales and a layer of them 30 feet above the level of the creek contains numerous specimens of: 1 Estheria sp. | (a) 2 Beyrichia sp. (2) These shales are in the Sherburne formation which as already described extends up the creek valley to Rensselaerville and down it to below its mouth on the Catskill. ; Red argillaceous shales occur on the road across the southern end of Pine Tree hill which forms the divide between Tenmile and Kelsey creeks, 160 feet above the level of Tenmile creek at the mill or 110 feet above the creek level at the first bridge north of the mill: These shales were regarded as the base of the Oneonta formation and occur at the same position as represented Es Se on the Geologic map of New York. From the base of the red | shales to the top of Pine Tree hill on the road toward Medusa there are 95 feet of red shales with some greenish layers. Near the ‘‘ pine tree” on the road across the southern end of the hill one half mile northeast of Oakhill there is an outcrop of red 268 NEW YORK STATE MUSEUM shale some 220 feet above the Catskill creek level in Oakhill. _ This exposure is apparently about 100 feet above the base of the Oneonta, but the rocks are covered by drift along the road down the western side of the hill. ! LVII A’ At Oakhill Kelsey’s creek flows into the Catskill from the north. In the lower part of the glen just above the, street bridge and 15 feet above the level of Catskill are blue, argillaceous shales which contain specimens of Hstheria sp. apparently the same as those found at the foot of Felter’s falls in Rensselaerville township. Higher in the glen are green argil- — laceous shales, which belong in the Sherburne formation that extends up this creek for a distance, and greenish sandstone with some that is dark gray in color. Loose pieces of red sandstone were also noticed in the upper part of the glen. It is reported by some of the residents of Oakhill that natural gas comes to the surface just above the street bridge in Kelsey’s creek. Red shale and sandstone show on the highway three fourths of a mile north- west of Oakhill not far below the first cross road across the creek, and about 225 feet above the -level of the Catskill in Oakhill. On the cross road is an outerop of red shale with some — that is green in color 115 feet higher than the creek at Brown’s” mill. Red sandstone forms a ledge on the western bank of Cats- kill creek rather more than three fourths of a mile above Brown’s mill and not far below Cooksburg. This ledge according to the contour lines on the “ Durham sheet ” of the United States topo- graphic map has an altitude of about 740 feet above sea level. From this locality the base of the red rocks were followed south- easterly along the western side of Catskill creek. In the brook below Durham village the lowest red rocks seen are shales which occur at an elevation of 720 feet A. T. Below this outcrop the rocks are mostly covered along this brook and this shale may not be at the base of the reds. In a small brook entering the Catskill from the west at Eagle bridge and mill, one mile below Oakhill are red shales only 30 feet above the level of the creek and below them along the brook and on the bank of the creek are bluish and olive argillaceous shales which are probably at the Bilis i. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 269 top of the Sherburne formation. The dip is 24° S, 60° E on the . bank of Catskill creek below the bridge. The red shales at this locality are considered to be the base of the Oneonta formation which does not extend much farther down the creek. On the Geologic map of New York the base of the Oneonta formation is represented about three miles farther down the creek near Hast Durham, but there are occasional exposures of the red rocks along the creek between the two localities. The bed of Catskill ereek east of East Durham is composed of red sandstone while on the western bank one mile above the East Durham bridge there is a ledge 25 feet high composed of red shales alternating with grayish and greenish shales and sandstones. There is a heavy dip to the SE along this part of the creek valley. , LVIIB On the western bank of Catskill creek just below the - highway bridge, a short distance south of Oakhill, are ledges 15 - feet in thickness (B1). These rocks are mainly greenish argillaceous, shales with some bluish shale and alternating with them are sand- stone layers. The sandstones are bluish to greenish in color and ihe fine greenish shales contain plenty of concretions of iron ‘pyrites, which in weathering stain them in spots and streaks a rusty color. Loose in the creek is a large conglomerate boulder containing some quartz but a much larger number of clay pebbles. The dip at this locality is about 3° S, 60° E; while directly south the rocks appear to lie nearly horizontal. In this region of south- ern Albany and northern Greene counties there has been appar- ently some gentle folding which is well obscured by the heavy covering of drift. No fossils were found in these rocks which are in the upper part of the Sherburne formation. Near the above locality a stream enters Catskill creek from the west which I have called Durham creek, and a section along this creek and highway from the creek through Durham and West Durham to the crest of the eastern line of the Catskills was carefully studied. The variaus outcrops found along this section are shown on the following diagram in which the altitudes are based upon the | contour lines of the ‘“ Durham sheet ” of the United States geo- logical survey. 270 _ NEW YORK STATE MUSEUM The rocks along the lower part of Durham creek are mostly covered; but about 80 feet higher than the Catskill creek level is an outcrop of red argillaceous shale (B2) in its bed. This locality is below Durham just beyond the house of Noah Scutt, where there is perhaps in all a 10 foot ledge with three feet of red shale at the base. This ledge ‘is in the red rocks of the. Oneonta formation near, if not quite at, its base, and is appar- ently at the same locality at which the base of the Oneonta form- ation is represented as crossing this creek on the Geologic map of New York. A little higher below and under the viaduct just east of Durham village are 23 feet of bluish sandstone with some greenish argillaceous shale partings. No fossils were found in these rocks. The dip varies considerably in amount even in a short distance, as for example at the base of this outcrop it is about 4° to the SW and 2° S, while above the viaduct it is 54° S. It is rather difficult however to determine the amount of the dip accurately on account of some irregular bedding in the rocks. On the highway about one mile west of Durham are coarse grained, irregularly bedded, grayish to greenish gray sand- stone in thin layers, 30 feet or more of which are exposed. In the upper part of this outcrop some 550 feet higher than Catskill creek is a thin layer of bluish sandstone (B*) containing fossils. The list is as follows: | : 1 Spirifer mucronatus (Con.) Bill. (c) Small specimens. 2 Orthothetes chemungensis var. arctostriatus (Hall) H. & C. . (a). 3 Tropidoleptus carinatus (Con.) Hall ! (r) 4 Homalonotus dekayi (Green) Emm. (rr) 5 Nuculites triqueter Con. : (rr) 6 Chonetes scitula Hall (c) 7 Palaeoneilo constricta (Con.) Hall (rr) Above the fossiliferous layer is a thin stratum of conglomerate possibly one foot in thickness. This outcrop is by the roadside just below the E. A. Moss house one mile west of Durham village, opposite the 25th mile post and a little below the crossroad to the OLIN oor Orr oos oot STHASLYINGILIYS FHL SO LEFYI FHL OL | WY LEM MH LH LS 009 IW HYD M0779 ; va ALTE) HASLLI WOES WOIL ITS l a = 009 00 D0e/ 00// WHHYAT SO LSPA WNL LNOBY FNOLSONKS AVE GQ SETS OL Oez/ ee £G *"FNOLSONYS H/ STISSOS*AIWHS ONY Dixryzwo7ane) * FINOLSONYS (8S SED EIESIO 014 00F/ 0av/ VLNOINO 5 TWHS NIIVYO He ot I Sikes ey We, 37s O94 Sa, 109/ DIVHS NIZE9 ONG OBY = EE 699 fe , ‘FIV OMY = OSS SS oy J DOLs HIYDHD WEY, 008/ INOLSONYS REESE 000/ = = = = IPA DG 48704 AO LSIN SHOAL OOOH over ey gh + SONVS HIINDTHD bu oLsONeS FINDS! F7VHS O2¥ amie |\NOLYVT ore $F +0 BEROb/E INOLSONYS HSIN IUD INDAWFIHI go 2WHS OFY BEE 0/ LE FNOLSONUS “WSINFIUD “vo NOLLIS YS VEZITVNS RINOLSONES OFY 4 TNIVW gf ooer iW, NV. oF, “pede SETA SSAA ITS APD ARS (bbe THM 40 cOLNO FTWHS CIY'TTIWSLVD ose ra WLNOFINO 70 FEHB" FTIWNWS OFY “WEHYAGD MOIFID LIN0V/A 4H ACN FNOLSONWS AvVieng WHHE?DO a dy FINI 77/MELYD NO +94 40 GHASOIX ZF — ———— CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 271 south. Loose shales were also found at this place which contain a fair number of fossils, apparently Hamilton species. Perhaps the shales are from a boulder though they are lumpy as though they had not been transported very far. The fossiliferous layer described above occurs 475 feet higher than the red shales of B? in the creek below Durham. Red shales and sandstones are conspicuous at various localities on the west- ern side of Catskill creek below this fossiliferous bed and all of that region is colored as in the Oneonta formation on the Geologic map of New York. This classification has been accepted by the author for the purpose of geological mapping for, on account of the almost entire absence of fossils it would be next to impossible to draw a line separating these formations unless some prominent lithologic character like the first appearance of the reds be select- ed for such purpose. Such a line is not a continuous one for it represents horizons of somewhat different geological age at differ- — ent localities, but perhaps it is as good a method as can be de- vised for the separation of these rocks. It seems to the author that this lentil of fossils 475 feet above the base of the reds shows conclusively that the reds in Albany and Greene counties ap- peared near the close of the Sherburne and practically replaced the Ithaca formation by rocks which are indistinguishable from those of the Oneonta formation. On the road 815 feet higher than Catskill creek are greenish argillaceous shales containing fragments of plant stems. Greenish and reddish shales, the reds rather arenaceous, occur 75 feet higher. At the base is a grayish sandstone and the entire outcrop is 25 feet in thickness.. This locality is on the road just east of the stone schoolhouse and one mile east of West Durham. At the forks of the road just west of West Durham and the cemetery are coarse, greenish sand- stones alternating with red and green shaies, 1330 feet higher than Catskill creek. Glacial striae show very well on top of the greenish gray sandstone running about W, 10° N, and E, 10° S. Below the fork toward West Durham there is greenish sandstone alternating with reddish shale, but for 50 feet or more the sand- stone predominates. Just above the fork on the road turning ee a We NEW YORK STATE- MUSEUM south is a good exposure of red shale. On the Geologic map of — New York the base of the Chemung is represented as crossing the highway just above this fork which is 1260 feet or more above the lowest reds seen in Durham creek. This would give a thick- ness of 1250 to 1300 feet for the Oneonta formation. Above the road fork on the southern road'there are 120 feet of nearly con- tinuous outcrops of rocks which are mostly reddish shales with -gome greenish streaks. Lithologically they are not different from the reds of the Oneonta below or those of the Catskill above. On account of the supposed Chemung age of the rocks for the succeeding 250 feet the outcrops from this fork to the Sutton gap were carefully examined by my assistant in the Greene county field work, Mr R. B. Rowe, and myself. As already stated, from the top of the greenish sandstones at the road'‘forks 1990 feet A. T., for 120 feet the rocks are mainly red shales, as shown on the south road, on the western road at 2140 feet A. T. is red shale which contains.the branching plant- like form not uncommon in the Catskill rocks. This is succeeded by massive gray sandstone which is partly covered in the field but apparently extends to 2210 feet A. T. with a stratum of red shale near the middle of the zone. About 55’feet higher is the Sutton gap pass which on the Geologic map of New York is represented as at the base of the Catskill formation. The position and char- acter of these rocks which have been referred to the Chemung are well shown in B? of the accompanying ‘section. Mr Darton described these so-called Chemung rocks as follows: “ This mass becomes harder and coarser eastward and was traced ‘to and along the eastern front of the Catskill mountains, its base defin- ing the upper limit of the Oneonta formation. Its thickness aver- ages about 250 feet. It is overlain by a red shale bed 25 to 30 feet in thickness and this in turn is overlain by the thick mass of hard, gray sandstone on which the old Mountain house is built. At a point about four miles due west of' Durham some molluscan remains were found in a softer gray bed about 175 feet above the Summit of the Oneonta formation. One fairly distinct individual 2940" A Ce EOD SANDSTONE is LIZ SA LIOO SL CTION UF MOUNT PIS GAL, SUUTHELN SIDE No.5 /, 6. ree LEZ Hh 2700 FLAGGING : BLVISH Ta FE DD/S H SANDSTONE. Cl? 2680 = 2600 25004 SE eee: '. SLUISH ANDO 6REENISH-GRAY COARSE SANDSTONE, cé CATS ATLL 2400 “se MEAVY 6REENISH- GRAY SANOSTONE. GC? 2300 é ¢ 2200 _ FEO SHALE WITH ARENACEOUS LAVERS, -6REENISH-GRAY SANDSTONE ct Ke, 2/00 Gt AASO = = =< =an Ogee NISH=- 6 FAV PAASS/IVE SAMOSTONE. 3 CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 273 was recognized by Dr Hall as Spirifer disjunctus, a Chemung form.’ In our search we were not successful in finding fossils in this” zone except Lepidodendron sp. and fragments of plant stems. It is very evident however that there are no 250 feet of coarse, gray sandstones, but in the upper half of the zone are heavy layers of grayish to greenish gray sandstones alternating with red shales and sandstones. The lower half of the zone is composed largely of red rocks, but in the upper half there are two heavy ledges of the greenish gray sandstones separated by red and green shales with a thickness of from 70 to 80 feet. On the hill to the south of the pass the rocks are largely red shales and sandstones with 3 some layers of greenish sandstone. This hill is mapped as in the lower part of the Catskill formation on the Geologic map of New York and it has an approximate altitude of 2490 feet A. T. LVII C. To the southeast of the point just described on the southern side of Sutton gap is Mt Pisgah, at the corner of Cones- ville and Durham townships, which is given as 2885 feet A. T. on the “Durham sheet.” of the United States geological survey. For my barometric section I obtained an altitude of 2940 feet A. T., but the readings were probably affected by rain. Guyot gave its altitude, determined by the barometer, as 2905 feet. The ac- companying section of the southern side of Mt Pisgah gives the relative position and thickness of the prominent ledges shown on its flank. Not much above the highway on the south side of the © mountain are two conspicuous ledges of massive, greenish gray sandstone, the lower one (C®) 30 feet thick with red sandstone on top, and the upper one (C*) 15 feet thick above which is red shale. The dip of this sandstone is between 34° and 4° 8S, 30° W. On the Geologic map of New York the area of these sandstones is colored as in the Chemung formation and it is probable that they are stratigraphically in the upper part of the zone called Che- mung on the Catskill turnpike to the north, though the heavy dip to the south would carry those sandstones rapidly below the altitude which they have on that highway. For the succeeding a Amer. jour. science, 3d ser. 1893. 45:207. OTA: NEW YORK STATE MUSEUM part of the mountain there are ledges of greenish gray and bluish | a < sandstones alternating with red sandstones and shales, while the e z red rocks predominate in the upper 450 feet. No fossils were found in any of the outcrops and they certainly agree in litho- Se a logic characters and stratigraphic position with the rocks of the Catskill formation. Eastern townships The eastern townships of Greene co. from the north to tie sede south are New Baltimore, Coxsackie, Athens and Catskill, while Cairo lies to the south of the western part of Coxsackie and west - of Athens. The lines separating the Hamilton and Sherburne and the Sherburne and Oneonta formations have already been : described across New Baltimore township and they will now be traced to the south across the county. Along the Cabin river from Grapeville in the western part of me New Baltimore township to Urlton in the western central part of Coxsackie township, there are numerous small, rounded hills composed largely of soil, gravel and boulders, between which are marshy and swampy flats. The rocks are mostly covered by these drift deposits so that it is a difficult region in which to trace the boundaries of geological formations. : LVIII A! On the bank of a small brook one fourth mile south- east of Urlton are blue fossiliferous shales in which typical Hamil- ton fossils are abundant. The fauna is as follows: 1 Chonetes coronata (Con.) Hall (a) 2 Spirifer mucronatus (Con.) Bill. (c) 3 8. granulosus (Con.) H. & C. (rr) : 4 Goniophora hamiltonensis (Hall) Miller . (r) 5 Orthonota undulata Con. (r) 6 Nucula bellistriata (Con.) Hall (rr) 7 Nuculites oblongatus Con. Ad (rr) 8 Limoptera obsoleta Hall (r) 9 Actinopteria boydi (Con.) Hall (rr) 10 Tentaculites bellulus Hall a ee These rocks are indisputably in the Hamilton formation. The ~ dip is 44° to the SW, while on the northern point of Coleberg hill 4 3 STTINSLVO NUMHLUON AHL JO HVDSIg LN OT 9}8Td : Sa CLASSIFICATION, HTC. OF HAMILTON AND CHEMUNG SERIES 275 to the southeast there is a dip varying from 6° to 9° N, 80° W. The increase of the dip is apparent as one goes eastward toward the folded ridges which become more conspicuous farther south in Athens and Catskill townships. Southeastward the Hamilton formation is found at the summit of the highway where it crosses the northern end of Coleberg hill. On the hill to the west of the East Branch Potuck and about one mile west of Urlton are green and red shales. The outcrop is on the road toward Result and west of the first road turning north on the western side of the West Branch Potuck. The shales are argillaceous and above them is reddish sandstone. On the Geologic map of New York the base of the Oneonta formation is drawn at the three corners west of Result, two and one fourth miles west of this locality. There are other outcrops of the red rocks along this highway to the east of the region mapped as Oneonta, and on the hill to the east of Result is a massive ledge of red sandstone. : LVIII B! Two miles south of Urlton the East Branch Potuck and West Branch Potuck unite forming Potuck creek. One fourth mile to the west on the Gayhead road is the Baker flagging stone quarry where a ledge 10 feet thick has been opened. Itis a blue sandstone making fair flagging and the flags contain a fair num- ber of specimens of Spirifer granulosus (Con.) H. & C., Camarotoe- chia congregata (Con.) H. & C. and Palaeoneilo constricta Hall (?). This sandstone ridge is evidently in the Hamilton formation though near its top, for at the four corners three fourths of a mile to the west are red argillaceous shales which continue to the west along the Gayhead road across the northern end of Indian ridge. : To the east of the Potuck creek it is very rocky and rugged, making an extremely poor farming country. The rocks of Potuck hill and the smaller ridges to the west on the eastern side of the creek apparently belong in the Hamilton formation, which in this region is composed mainly of sandstones and coarse, arenaceous shales. From Urlton the top of the formation ap- parently follows the valley of the East Branch Potuck and gana end of Potuck creek the rocks dip about 8° W. Te In the gorge of the Potuck at the Potuck mill about one ote at the base and in the upper part of the banks are bluish shales _ and sandstones, some of which show very good examples of rip- _ 2 ple marks. No fossils were found though careful search “was made for them, and the dip is 8° W. These rocks apparently bes long in the Sherburne formation and this conclusion is supported x by the presence of red shales 215 feet higher on the steep, eastern a side of the southern end of Indian ridge. Red sandstone and Shales outcrop at the three corners at the southern end of Indian — ridge 145 feet higher than the outcrop mentioned on the eastern rs slope. On the road down the southern end of the ridge from the = above three corners there are several outcrops of red shale, the oe lowest one only 65 feet above the level of the Catskill creek road. Red argillaceous shales with red sandstone above are shown on ~ the northern bank of the Catskill creek below the place at ‘ile : the highway turns toward Cairo. The Sherburne formation does. wee not extend much farther up this valley and it is at about this point that the base of the Oneonta formation is represented as . | crossing the creek on the Geologic map of New York. | Eig On the bank of a small brook entering Catskill creek from the cm south one half mile above South Cairo are red argillaceous — | shales and sandstones of the Oneonta formation. Above ae reds are coarse, gray to bluish sandstones which dip 8° 8, 20° ES Farther west toward Cairo a prominent ledge of sandstone, on which glacial striae are nicely shown running a little E of 8, crosses the highway. On the southern bank of Catskill creek one and one fourth miles below South Cairo and nearly opposite te Potuck creek are green argillaceous shales and sandstones below which is very hard, coarse grained, greenish to reddish sandstone . Z with some red argillaceous shales. The dip is from 34° to 5° N, oy ‘ 70° W. This variation in the direction of the dip noted at dif- ferent places along this part of Catskill creek shows that the rocks are gently folded in this region. at a> — Ps ss ‘<- ‘sab 2 oe ‘ ) Power’ \ - eee eK, : - “REA OD t ciel orl & ¥ a = ma ey oe > a DEED Na Ate op Haig nme Ee a ei _ . Py Saree s ANOLSAWIT ATVHS LYVd YAMOT ‘AIVHS SOdAOSH ANIIOILNV WO LUVd Ydddf) SdWa]T MOTH MAAYO TTIMSLVO NO anto¥4 Nara set eS a BA ey tet eae ers. * % : ~ CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 277 LIX A! In the highway and railroad cut just above the toll gate one mile above Leeds are blue fossiliferous sandstones and shales. ~The rocks are greatly indurated and on weathering much stained by iron. The strata show a small roll and the locality is about opposite the western base of Potuck hill. The formation is clear- dy the Hamilton as is shown by the following fauna: 1 Tropidoleptus carinatus (Con.) Hall (a) 2 Chonetes coronata (Con.) Hall . (aa) 3 Camarotoechia sappho (Hall) H. & C. (?) (rr) 4 Paracyclas lirata (Con.) Hall | (r) 5 Nucula bellistriata (Con.) Hall : re fce 6 Prothyris lanceolata Hall (rr) 7 Grammysia sp. | (rr) In the Catskill creek above the falls at Leeds and farther up | are outcrops of the Onondaga limestone while to the west the Marcellus shale is not exposed, being covered by the deep soil of the creek valley. The precipitous and rocky Vedder hill rises on the western side of the Catskill creek valley to the southwest of Leeds, the rocks of which belong in the Hamilton formation. In fact the exposures in the railroad cut at LIX A! are at the north- - ern end of this hill where it is terminated by the Catskill valley, but the hill is really continued on the northern side of the creek by Potuck hill. On the road leading southwest from the toll gate up and along the western slope of Vedder hill the Hamilton fossiliferous shales were seen at an outcrop 70 feet higher than the one in the railroad cut, while at a point 160 feet higher is a ledge of bluish sandstone with some that is coarse grained, gray- ish, and very hard. Before reaching the summit of the highway, about 215 feet higher than the railroad cut, a ledge of red, argil- laceous shale crosses the road which was considered the base of the Oneonta formation. | At the three corners two miles east of Lawrenceville are red shales. In the Bloom quarries in that vicinity the stone is some- what striped bluish to bluish gray sandstone which splits in thick layers. Between the lower and upper quarry ledges are greenish stones but into thicker layers. These stones are heeds than th ae pomuton flags and they are oe into pecs Sade paving. ‘No fos burne formation. At the place aiere the Uawnentevii - crosses the small brook which is followed down the eastern si of this ridge into the Kaaterskill creek valley are typical aly Hamilton shales containing characteristic fossils. 3 1 Spirifer granulosus (Con.) Hall” 2 Palaeoneilo constricta Hall | 3 Grammysia alveata (Con.) Hall : 4 Schizodus appressus (Con.) Hall. atu 5 Elymella nuculoides Hall — 6 Pleurotomaria sulcomarginata Con. 7 Bellerophon lyra Hall 8 Spirophyton velum Van. This outcrop is some 300 feet higher than the Kaaterskill creek which flows northeasterly for five and one half miles at the east- ern base of this steep ridge. The greater part of the Kaaterskill valley for this portion of its course has been cut out of the com- _ paratively soft Marcellus shales which are shown on the eastern | bank south of the bridge on the road from Catskill through Kis- | . katom to Palenville. The western side of the ridge to the east | of the creek is composed of the Onondaga limestone, the distri- — 3 bution of which is well shown on Prof. Davis’s map of “The folded. ; : Helderberg limestones in Greene county, N. Y.’% The rocks to the west of this bridge forming the fat terrace _ are no. 132'of Mather’s section from Catskill mountain to the eo creek which he described as “ ae shales and chal a Bulletin Museum comparative zoology, v. 7, Geol. series, v.1, no. 9, 1883, pl. 13. MNAM # de ST 9+?ld oe rs %. CLASSIFICATION, BTC. OF HAMILTON AND CHEMUNG SERIES 279 a from the Ithaca group to the Marcellus shales.”* In another place he states that “This part of the series can be examined satisfactorily only by following up the bed of a stream near which the turnpike passes. These strata are probably 1000 feet in - thickness.” oat _ On the roads to the west of Kiskatom are numerous outcrops of red shales and some sandstones. On the road to the south leading down into the Kaaterskill valley are massive, hard sand- stones with banded structure which are in the Sherburne forma- tion. In a small quarry some 35 feet lower are massive sand- _ stones which split into thick layers. Plenty of'plant stems were | found in these rocks but no other fossils. The dipis 8° N 60° W. At the three corners of the road a little lower than the quarry are blue shales containing Hamilton fossils, consequently it ap- pears that the sandstones in the quarry are near the dividing line between the Hamilton and Sherburne formations. LX Aiand2 At the High falls’ on the Kaaterskill creek not far ‘from the Greene and Ulster county line is a deep and rocky gorge in which the upper Hamilton rocks are finely shown. Below the massive sandstone stratum which forms the bed of the creek _ above the falls are rather fine, blue argillaceous shales (A?) which contain a fair Hamilton fauna of the species usually found in the. fine shales of that formation. The following species were col- lected from these shales: 1 Tropidoleptus carimatus (Con.) Hall (c) 2 Chonetes coronata (Con.) Hall (c) 3 C. lepida Hall . (rr) 4 0. setigera Hall 3 (r) 5 Strophalosia truncata (Hall) Beecher (2) (rr) . Imperfectly preserved. 6 Spirifer mucronatus (Con.) Bill. (rr) ey granulosus (Con.) H. & C. } (c) 8 Stropheodonta perplana (Con.) Hall (rr) a Geology of New York. 1843, P. 1, p. 305. b Ibid., p.306. ce Also called ‘* Great falls.”’ oe oA “them is a ae sandstone (A2) between three mad four ioe - (2260. © - erotalum Hall (?) 9 Palaconeilo emarginata (Con) Hall 10 P. ~*~ constricta (Con.) Hall 11 Nucula bellistriata (Con.) Hall 12 N. - varicosa Hall “13 Nuculites triqueter Con. 14 Paracyclas lirata (Con.) Hall ere 15 Orthonota (?) parvula Hall | Le A ae 16 Modiella pygmea (Con.) Hall. : Ue ag “17 Sphenotus truncatus (Con.) Hall : ee 18 Nuculites oblongatus Con. ; Tee Pee — 19 Solen (Palacosolen) siliquoidea Hall (?) tag & | 20 Prothyris lanceolata Hall 25 ee ae 21 Grammysia constricta Hall AO a | 22 Schizodus appressus (Con.) Hall oe 23 Mierodon (Cypricardelia) tenuistriatus Hall 8 24 Liopteria dekayt Hall — : is se 25 Orthoceras subulatum Hall (ON ae a : a 27 Pleurotomaria sulcomarginata Se (?) (28 Bellerophon sp. Fragments. 29 Dignomia alveata Hall (?) : 30 Lingula sp. (Broken) oe ds ae 31 Crinoid stem (Large) : thickness, which splits in irregular layers. ‘The upper part this sandstone contains an abundance of the species usually oe found in the coarser Hamilton deposits as for example: 1 Spirifer granulosus (Con.) H. & C. : Zi. mucronatus (Con.) Bill. : 3 8. audaculus (Con.) Whitt. : 4 Tropidoleptus carinatus (Con.) Hall Plate 19 IKAATERSKILL FALLS. CATSKILL AAT aaa 4 it i . 4 ye P we £ : . # [) be « a we 4 ti E vw oo ot , i 7 : 7 Ua pan : aay ; 1 f f j= CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 281 yo 5 Chonetes coronata (Con. Hall 6 Strophoedonta perplana Con. (?) Grammysia bisulcata (Con.) Hall 8 Spirophyton sp. ete. The dip above the falls is 104° N. 60° W. The western bank -of the creek above the falls is composed of alternating strata of shales and sandstones forming a perpendicular cliff 85 feet in hight. It was not possible to determine whether the Hamilton fauna continues to the top of the cliff or not. The fossiliferous nature of these rocks was noted by Prof. Davis who wrote that “several strata are very fossiliferous, Spirifer. mucronata and medialis are both of common occurrence; while Prosser has in | earlier papers-partially listed the fossils of this locality.® 7 ; On the hill one half a mile west of High falls and 1380 feet - higher than its top is the small stone quarry of Hugh Smith. The rock is bluish gray, rather coarse grained sandstone which has bands of color, some of it with a slightly reddish tint in the bright sunshine. The sandstone is capped by a mass of green, argillaceous shales with some layers of bluish color. No fossils were found and it is this part of these rocks which I have re- ferred to the Sherburne formation. The soil in this vicinity is reddish from the leaching of the higher red shales. The first . reds seen in place however are at the three corners, three fourths of a mile farther northwest on the ridge east of the Kaaterskill. This locality is just south of the Greene and Ulster county line about one and one half miles east of Palenville. Some of the red shales are very arenaceous and it is quite probable that the base of them is somewhat farther east, but covered by drift and soil along the highway. Red shales show at various places along this ridge and the highway to the south of Saxton in Saugerties township, Ulster co. On the geological map accompanying this report the lines separating the Hamilton and Sherburne formations and the Sher- burne and Oneonta are indicated as nearly as we could follow a Bull. Mus. comp. zoology, v. 7, Geol. ser. 1883, 1: 312. 5 American geologist, 1891, 7:365; Bulletin Unite ‘gs geol, survey, no. 120, 1894, p. 69. - 2 ae | NEW YORK STATE MUSEUM ~ them across this county. Itisa difficult region to map and in places the indicated lines are probably only an approximation. In the above account the localities at which the outcrops near the dividing lines occur have been described so fully that it is 2 not deemed necessary to define the course of these lines and all : interested in their position may follow them readily on the geo- — logical map. Greene county Catskills The western and central portions of Greene county are in the aor Catskill mountain region, the rocks of the greater part belonging ae in the Catskill formation for which it is the typical region of the — “ Catskill division ” as they were called by Mather. His detailed section “from the top of the South mountain near the Mountain house on the Catskills, down to the Helderberg division at the — Kaaterskill creek,”* gave the rocks of the Catskill and Erie divis- ions? and extended from the eastern part of Hunter northeasterly across the southern part of Catskill township to the Kaaterskill creek. In 1874 Mr Andrew Sherwood measured very accurately a sec- tien of these rocks beginning in the Kaaterskill creek at Palen- ville, following the famous Kaaterskill clove and continuing to the top of Round Top mountain to the south of the clove®. Sherwood’s total thickness for the rocks from the upper part - of Palenville to the top of Round Top is 3482 feet, while Prof.. _ Hall estimated the thickness of all the rocks from the top of the Hamilton formation to the summit of Round Top as 5800 feet. Sherwood gave accurately the lithologic characters and thickness. of the various strata so that there is no need for another de- tailed account of this typical Catskill section. Sherwood cor- related the red and green shales (no. 94 of his section) in the a Geology of New York. 1848. P.1, p. 302-5. b “The Erie division in the first geological district consists of the following groups: .1 Ithaca and Chemung group 2 Hamilton group 3 Marcellus shales.” Ibid., p. 317. c Proc. Amer. philosophical society, 1878, 17:346-47. This section was also republished by Ashburner in the Second geological survey of Pennsylvania, F. 1878, p. 218-19, while Prof. James Hall has given an account of it in the 28th Report N. Y. state museum of natural history, 1879, p. 14-15. d Proc, Am. ass’n adv. science. 24:82, 83. SNIVINOOW AVELVId GNV YOLINOW NEWMLAA SsVd AHL ‘MAOIO ANOWLS Hosm¥No yous i 7530 OG 342Id + ee Sart ea “ha OW tea tale | ing CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 283° Kaaterskill creek above the bridge opposite the hotel in the upper end of the village, with the red shaly rock (no. 12) at the top of the Manorkill cataracts near Strykersville. The author did not see any evidence to support this exact correlation of these- two sections, nor did Sherwood give any reason for his correla- tion. But few fossils have been found in the rocks, the animal remains in which are bones and plates of fish that were first dis- covered by Sherwood, and on account of their presence in con- siderable abundance in three layers (nos. 105, 107 and 111) in the lower part of the clove he termed them “ fish-bone beds.” The lower bed is in a greenish, shaly rock which is quite hard, and there are numerous fragments of fish bones and plates most of which are badly broken. The setond bed is in a mottled red and “green argillaceous and rather soft shale. The bed of no. Lil is. “near the bottom of a mass of red shale, 103 feet in thickness ac- cording to Sherwood, where fragments of fish scales were seen, but they are not nearly so abundant as in the two lower beds. These specimens were not identified, so far as known to the writer, except that Prof. Hall referred to these beds, stating that — they were “charged with the remains of Holoptychius.”% 5 Pleurotomaria sp. (in ee These rocks along the creek into the valley of Esopus creek are in the Hamilton formation. On the south bank ofthe Esopus creek at the Hudson river pulp mili two and one half miles below ~ Olive city are massive, greenish sandstones which form a rocky — : a gorge and are apparently in the Sherburne formation. Loose in “a some bluish argillaceous shales are specimens of Hstheria sp. apparently identical with those found near Oakhill. ‘To the northwest of this hill no reds were seen on the road from Esopus creek to Olive branch. ; , The upper line of the Hamilton formation crosses the Ulster — and Delaware railroad a short distance west of Bristol chureh, Re sites then is followed with difficulty across the rugged central part of :: a CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 299 Hurley township, crossing Esopus creek below the Hudson river pulp mill, and then runs across the western part of Marbletown into Rochester. On the hill south of the Esopus creek about two and one half miles west of Marbletown are bluish, concretionary sandstones which are not far below the blue sandstone quarries at the three corners where one road turns to the south. The upper part of the sandstone ledge is heavy and crossbedded, below which are guite extensive flagstone quarries in bluish gray. sandstone which alternates with bluish and greenish argiilaceous Shales. The dip is from 34° to 4°N, 50°E and the quarries are in the Sherburne formation. Not far below the quarries are 7 coarse, arenaceous, blue Hamilton shales in which are some fos- nie _ Sils, as Chonetes coronaia (Con.) Hall and fragments of a few other species. These shales are near the top of the Hamilton and some 295 feet below the base of the lowest reds on the hill above. This section gives the approximate thickness of the Sherburne forma- tion at this locality. At the northern end of the Lynesville pond about one and a half miles nw of Kripplebush is a small quarry in bluish Hamil- ton sandstone alternating with bluish shale, in which are Ham- | ilton fossils, Camarotoechia congregata (Con.) H. & C. and Ten- taculites spiculus Hall. Some of the rock contains quartz peb- bles. To the west of Lynesville is the steep Mackey hill which is some two miles northwest of Kripplebush. On top of the hill are thé Mackey flagging stone quarries, some of the stone being bluish gray in color and some banded grayish. The sandstone is in rather coarse layers and does not split into thin flags. It is capped by a considerable thickness of bluish argillaceous shale in which no fossils were found. There is a stratum of conglom- erate six inches thick in which are red, black and various colored pebbles. The dip is between 4° and 5° N, 30° E. In the some- what shaly partings are fossils, as Spirifer mucronatus (Con.) Bill., Chonetes coronata (Con.) Hall; Camarotoechia congregata _ (Con.) H. & C.; Tropidoleptus carinatus Hall; Chonetes setigera Hall; Prothyris lanceolata Hall and Crinoid stem, and the rocks are apparently in the Hamilton formation though near its top. ~ 300 NEW YORK STATE MUSEUM pe To the south of Mackey hill along the highway near Whitfield are ; ae : fine blue Hamilton shales belonging in the lower part of the formation. A To the east of Tobasco and two and a half miles south of ea Samsonville are the Gray quarries. The dip is 54° N, 80° W. The rock which alternates with greenish shales is a coarse, bluish See gray, quite massive sandstone, which does not split into thin ‘shales, and which shows crossbedding on the edge of the ledge. = i : No fossils were found and the quarries are in the Sherburne ee formation. The base of the red rocks on the hill south of Esopus creek runs southeasterly for several miles to the hill east of Krum ~ ex corners, when it turns westerly toward Samsonville. This carries the Catskill formation somewhat farther east than is indicated on the Geologic map of New York and the valley to the ~ : west of Krum hill is in this formation instead of a lower one, for — on the highway just north of Krum corners or Krumyille church - are red and green mottled, argillaceous shales. On the low hill just east of the road and 55 feet higher is a small quarry of _ ; _ coarse grained, bluish gray sandstone which splits into flags. There are partings of bluish, argillaceous shales in which are ze fragments of plants. The edges of the outcrop show cross- bedding. The dip is 6° N, 70° W, and on another face of the quarry 2° N, 30° E. Near the corners where the first road north of Krum corners turns to the east are red shales which’ are to — the southwest of the high hill shown as Catskill on the New York map. To the west of Krum corners is the Krumville postoffice and one quarter of a mile to the west on the bank of a brook is a quarry of bluish sandstone, some of the layers showing a red- dish tint. There are plant fragments but no other fossils were found. The dip is 4° N, 70° W, and the quarry is near the top of the Sherburne formation for red sandstone apparently in place occurs on the highway to the west of the brook near the line indicated as the base of the Catskill formation on the state map. — In Samsonville are conspicuous ledges of coarse grained, ereenish to greenish gray sandstone which have a decidedly crossbedded = CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 301 structure. These sandstones are specially conspicuous along the Rochester creek near the site of the abandoned tannery and they are near the base of the Catskill formation. Along the highway en the northern side of the creek one mile below Samsonville are outcrops of red and green shales, and above them is a heavy ledge of bluish sandstone in which a.small quarry has been opened. | : The base of the Catskill formation runs southwesterly from Sanmsonville, but it is difficult to follow the line closely on ac- eount of the heavy drift and infrequent outcrops. Along Mill: brook above Mombaccus the country is well covered with drift and beds of sand and gravel. An occasional ledge of grayish sandstone is shown and near the head of the stream are loose pieces of red shale which apparently have not been transported far and probably came from near the base of the reds. Below Mombaccus the country is also well covered with drift and soil so that outcrops of bed rock are infrequent. On the eastern side of the Vernovy creek a little north of Wawarsing are fine Hamilton shales containing some fossils. The dip is very heavy being 35° slightly west of north. The shales near the base of the first small hill are quite fine and fossils are common though not abundant. The species however are few, Liorhynchus and Chonetes being the most common. The _ list-is: 1 Spirifer mucronatus (Con.) Bill. is (rr) 2 Chonetes coronata (Con.) Hall (a) 3. Liorhynchus multicosta Hall (c) 4 Camarotoechia congregata (Con.) H. & C. (r) 5 Palaeoneilo constricta (Con.) Hall (rr) 6 Paracyclas lirata (Con.) Hall (rr) 7 Nuculites triqueter Con. (rr) 8. N. oblongatus (Con.) Hall (rr) 9 Nucula corbuliformis Hall (Ee) 10 Orthoceras constrictum Van. (rr) Near the top of this hill the rocks become coarser and irreg- ular; thin bedded sandstones occur showing a tendency to the - 302 Hamilton deposits. The fossils are rare in these coarser layers. About half a mile above Wawarsing just above saw mill are © sy coarse sandstones exposed by the side of the highway which - have a dip of 38° N, 40° W. They are bluish in color and split into rather thin layers. A little farther up the road is a conspic- uous ledge of bluish sandstone which splits into flagstones and a quarry has recently been opened in this ledge by the side of the highway. Ledges of red shale and sandstone cross the highway opposite the house of Mr Hillsdale, two miles above Wawarsing, about at the locality where the base of the Catskill is repre- oa sented on the Geologic map of New York. Several years ago a well was drilled in Wawarsing to the depth of 1776 feet, the — lower part of which is reported to have been in limestones. The lower falls of Rondout creek in Napanoch are composed of the fine blue shales of the Hamilton formation which also appear along the highway toward Ellenville. These shales contain a some fossils though neither species nor specimens are abundant. On the eastern side of Rondout creek just below Honk falls, — which are not far above Napanoch, are blue sandstones which split into rather even flaggy layers. The dip is from 40° to 42° N, 20° W, while on the western side of the creek it is not much more than 30°. The cliff on the western side is perhaps 100 feet high, in which are some massive sandstone strata four feet or more in thickness, alternating with thinner layers. No fossils — were found at the falls though the rocks are quite blue and in lithologic characters closely resemble the sandstones of the Hamilton formation. Not more than two miles above Napanoch on the eastern side of the creek the dip has decreased to about 12°. The first red shale seen in place occurs on this side of the | creek between the two bridges some distance above Honk falls. Along the valley road from Kerhonkson to Ellenville there is.a considerable amount of sand which also extends up the branches for some distance, as in the Rondout valley for two miles above Napanoch the roads on both sides of the creek are very sandy. NOLTINVH GHL UAAO “STIVA HOONVAVN AT Tis 6G ACI d _ CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 303 Red shales and sandstones outcrop conspicuously in the Beer- kill and on the highway a short distance above the fork of the creek to the northwest of Ellenville. Along the creek below and under the bridge over the western fork the red rocks are very prominent and this locality is near the line representing the base of the Catskill formation on the Geologic map of New . York. The older Devonian formations are not shown to any ex- tent in the vicinity of Ellenville. The dip is 20°N, 50°W. At various places along the highway from Ellenville to Homowack are exposures of Hamilton shales and sandstones, the latter oc- curing more frequently. Against the eastern foot of the hill just north of Homowack is a big sand and gravel bank below which is an outcrop of Hamilton shales. These shales are bluish, not very arenaceous and break into blocky pieces. Only a few fragments of fossils were found. A little farther up the highway, on the south side of Sandberg creek are bluish Hamilton shales which split into thinner layers than those first noted. The dip varies from 42° to 45°N, 50°W. Fossils, specially Lamelli- branchs are more common than in the lower shales, being abund- ant in some of the coarser layers. This is the best locality for collecting noted between Kerhonkson and Homowack, the follow- ing species having been obtained: 1 Nyassa arguta Hall | (a) 2 Palaeoneilo emarginata (Con.) Hall (c) tie op constricta (Con.) Hall | (r) 4 Grammysia constricta Hall - (rr) he cans alweata (Con.) Hall (c) 6 Cunitaria elongata (Con.) Hall (rr) 7 Glyptodesma erectum (Con.) Hall eat CEE} 8 Pierimea flabella (Con.) Hall (c) 9 Nucula corbuliformis Hall (rr) 10 Nuculites triqueter Con. . (c) 11 Goniophora hamiltonensis Hall (r) 12 Inopteria dekayt Hall (r) 13 Camarotoechia congregata (Con.) H. & C. (c) 14 Tentaculites beliulus Fall (rr) 15 Bellerophon sp. ov (rr) yy agen fae : fy pity 304 4 ‘NEW YORK STATE MUSEUM © argillaceous shales and some thick bedded, rather greenish sand- — is succeeded to the westward by the Hamilton formation. 16 Discina doria Hall 1% Athyris spiriferoides (Eaton) Hall 18 Modiomorpha subalata (Con.) Hall ) roe 19 Pleurotomaria sp. oe ce Above the bridge over Sandberg creek are decidedly olive — tiie rats ee stones apparently in the Sherburne formation. An outcrop of : a greenish blue flagstone by the highway two miles above Homo- — a wack has a dip of 6° N, 70° W. , hee SULLIVAN AND ORANGE COUNTIES Sullivan co. in southern New York which forms the New oe York border for the greater part of the cafion of the Delaware a river, is covered mostly by rocks belonging in the Catskill forma- | tion. The central part of Mamakating township however, the eastern township of the county, is crossed by the formations of the middle Devonian. In Orange co. the same formations cross Deer Park, which is its most western township, and enter Pennsylvania at Port Jervis. The strike of these formations is — about parallel with the course of the Basherskill and Neversink — river across these two counties, and in Pennsylvania with that of the Delaware for about 20 miles. In general the Marcellus shale is covered by soil in the valley of the Neversink river, and - Distribution of the Middle and Upper Devonian | Along the valley road from Homowack through Phillipsport — to Summitville the rocks are mainly covered with drift. By the side of the road a short distance north of Summitville re Hamilton shales which contain a few fossils. Exposed not far above the Wurtsboro hotel by the side of the highway are coarse, massive sandstones which are either in the upper part of the Hamilton or near the base of the Sherburne ~ formation. Crossing the highway less than one mile northwest | of Wurtsboro are red shales and sandstones which mark the base- of the Catskill formation. The dip is between 14° and 15° N, 70° CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 305 uh W. Above the red rocks are massive greenish gray or grayish sandstones and green argillaceous shales. Succeeding these rocks .is a prominent band of red argillaceous shale containing some green shale with a total thickness of between 40 and 50 feet. On the hill one and one half miles above Wurtsboro the rocks - are nearly all covered by drift for some distance along the road. By the side of the valley road over one half a mile southwest of Wurtsboro are fine, blue Hamilton shales, which contain some fossils, though they are not abundant. Perhaps one and one half miles below Wurtsboro is a good outcrop of these bluish, fine Hamilton shales, which contain but few fossils. The dip at this locality is 75° N, 50° W. In general this is the case with these somewhat blocky shales of the lower Hamilton as exposed along the valley road to the west of the Basherskill. The rocks along the Pinekill in the southern part of Mamakat- ing township for at least two miles above West Brookville are all covered by drift. The country is rough and there are large numbers of glacial boulders of various sizes. : On the hill just northwest of Cuddebackville are black argil- laceous shales in the upper part of the Hamilton formation, con- taining abundant fossils. The following fauna was. obtained from this outcrop: 1 Paracyclas lirata (Con.) Hall (a) 2 Nuculites oblongatus Con. (rr) 3 Nucula bellistriata (Con.) Hall (rr) 4 Tellinopsis subemarginata (Con.) Hall (¢c) 5 Modiella pygmea (Con.) Hall (r) 6 Leda rostellata (Con.) Hall (rr) 7 Nucula corbuliformis Hall (r) 8 Nuculites triqueter Con. (rr) 9 Modiomorpha mytiloides (Con.) Hall (c) 10 UM. subalata (Con.) Hall (?) : (rr) 11 Macrodon hamiltoniae Hall (rr) 12 Lunulicardium fragile Hall : (rr) 13 Spirifer fimbriatus (Con.) Hall : ; (r) AEST: web be meh ey Sy Stee bat St at Bigs wat vaca etn ie fee’ 806 _ NEW YORK STATE MUSEUM ~—_ 14 Ambocoelia umbonata (Con.) Hall - 15 Chonetes setigera Hall £6: Cie mucronata Hall (?) Aer i (rr) is 17 C. scitula Hall (2) | ee 18 Spirifer mucronatus (Con.) Bill. Ave See 19 Nucula randalli Hall (?) | eo eee 20 Dalmanites (Cryphaeus) booths (Green) Hall (tr) -S- 21 Phacops rana (Green) Hall . (rr) oe 22 Pleurotomaria sulcomarginata Con. (?) | Rees: ae 23 Bellerophon crenistria Hall (?) . es 24 Orthoceras crotalum Hall | . (rr) — 25 Grammysia sp. tee ce 26 Bellerophon sp. : ‘(eg Ea =: 27 (?) Lnopteria sp. (rr) te : 28 (?) Pterinopecten sp. | | =e ey 29 Crinoid stems The base of the Catskill formation crosses the Neversink river : just below Oakland. On the river bank at the lower Oakland _ bridge from 15 to 20 feet of red shale is exposed. At this locality : a well was drilled between 1300 and 1400 feet in depth, and according to Mr Case after passing through from 18 to 20 feet of ie ; red shale at the mouth no more was struck, the remainder of the __ well being in “ blue stone.” This shows conclusively that the red | a shales on the river bank are the lowest reds in this valley. Years ago a well was drilled 500 feet deep in the Bushkill valley, where — se it joins the Neversink at Oakland, the first 50 feet of which was in a clear blue clay. This clay is frequently shown along the Bushkill valley. At the upper Oakland bridge on the eastern side of the Neversink river is a cliff of greenish gray sandstone. and green and blue shale perhaps 75 feet high. No red shale : occurs in it though the rocks are above the red shales at the lower bridge and in the Catskill formation. aaeeer: In the small quarry at this place the dip varies from $° to1° - N, 20° E, while in the quarry a little farther down the road the rocks are nearly horizontal, though the upper part of the ledge — | is so badly shattered that this horizontality may not continue CLASSIFICATION, ETC. OF HAMILTON AND. CHEMUNG SERIES 307 for any considerable distance. In general the rocks are well 5 covered by drift along this part of the Neversink valley except on the steep bluffs, and boulders in large quantities have been Swept into it. At Rose Point on the Monticello and Port Jervis railroad is a - eut showing an excellent exposure of Hamilton arenaceous shales and sandstones. The dip varies from 40° to 45°N, 30°W. These shales contain abundant fossils and it is one of the best localities in the Neversink valley for collecting. The fauna is— as follows: 7 1 Spirifer granulosis (Con.) H. & C. : (c) 28. medialis Hall (?) (rr) BUS. mucronatus (Con.) Bill. 520) 4 Tropidoleptus carinatus (Con.) Hall (rr) 5 Nyassa arguta Hall oe (c) 6 Nucula varicosa Hall (rr) 7 Modiomorpha concentrica (Con.) Hall (rr 8 Chonetes mucronata Hall (r) 9 Camarotoechia congregata (Con.) H. & C. | (r) 10 Athyris spiriferoides (Eaton) Hall (vr) 11 Chonetes defiecta Hall (?) (rr) 12 Ambocoelia umbonata (Con.) Hall (¢). 13 Palaeoneilo emarginata-(Con.) Hall (r) 14 Nueula corbuliformis Hall (r): 15 Nuculites triqueter Con. (rr) 16 Palaeoneilo constricta (Con.) Hall (rr) 17 P. plana Fall (2) (rr) 18 Nyassa recta Hall ( ?) . (rr) 19 Modiomorpha subalata (Con.) Hall (2) (c) 20 Macrodon hamiltoniae Hall (rr) 21 Grammysia bisulcata (Con.) Hall (Er) 22 Homalonotus dekayi (Green) Emm. cde Jat 23 Dalmanites (Cryphaeus) boothi (Green) Hall (?) (rr) 24 Plewrotomaria sulcomarginata Con. or P. itys Hall — (c) 25 Bellerophon patulus Hall (?) possibly B. natator Hall - (rr) 26 Lozxonema delphicola Hall (rr) Pe Oe 5, <2 eer 3 Hi aie EARS ae 308 NEW YORK STATE MUSEUM 27 Orthoceras crotalum Hall ou ee ork 28 Conularia undulata Con. . : (urs ee 29 Lepidodendron gaspianum Du. (rr) Ee 0 (?) Psilophyton princeps Du. ae (rr). he _ 81 Pterinea flabellata (Con.) Hall : / | meee : “ 32 Actinopteria boydi (Con.) Hall ine oe 33 A. decussata Hall (?) | (rE Sy eS 34 Streptorhynchus chemungensis (Com) Hall cat (rr) ; | 5 35 Platyceras sp. Ee | 4 36 Two specimens of Pectinidae . ; : On the lower part of Prospect hill above Rose Point are : _ rather thin bedded bluish gray sandstones. In some of the eee a slightly shaly partings are fossils, a number of specimens closely : resembling Spirifer mesastrialis Hall, but the surface is so poorly ? preserved that the striae are shown only very faintly. The fol- | lowing species were obtained: 1 Spirifer mesastrialis Hall Re vce 2 Camarotoechia sp. : (rr). s 3 Lepidodendron ar . Along the highway somewhat higher are ledges of thin flaggy : stone which split into layers from one half to one inch thick. cee is The rock is of a slightly greenish tint, and very arenaceous and 7 4 fossils are common. The species mentioned in the following list oy were collected at this locality:. | 1 Spirifer mucronatus (Con.) Bill. (?) (aa) — 2 Tropidoleptus carinatus (Con.) Hall (a) 3 Palaeoneilo constricta (Con.) Hall (rr): 4 Oyrtina hamiltonensis Hall | (rr) 5 Microdon (Cypricardella) gregarws Hall (ec) 6 Paracyclas lirata (Con.) Hall (rr) 7 Modiomorpha subalata (Con.) Hall (?) (rr) 8 Actinopteria boydi (Con.) Hall (2) (rr) y 9 Chonetes mucronata Hall (?) (rr) 5 10 C. setigera Hall (ery ae SIAUGL LUOd AO BHINOS FHI OL S171 O90 0Y4O4MVYO WOSENATIVH dOOMNAM: i ” PZ OVI i). Leek eee Rieder See lt eee ne cee IN rie gk el SA hee AR var. chemungensis Hall (?) : (rr) 11 Liorhynchus sp. (rr) 12 Actinopteria boydi (Con.) Hall (a) 13 (?) Psilophyton princeps Dn. (r) 4 (?) Crania sp. or possibly Discina sp. GE) On the New York side of the river the rocks form a steep cliff 200 feet or more in hight at a place known as the Hawk’s nest. _ The dip as determined from the canal below is between 6° and 7° N, 10° E. No red rocks were seen in this cliff either from the canal or the Hawk’s nest road. On the hill toward Mongaup is a thick deposit of sand and the older rocks are well covered by it and drift. There is apparently another sand hill on the west-. ern side of the river nearly opposite the Hawk’s nest. On the Pennsylvania side just below ‘the Pond Eddy station is an ex- posure of 17 feet of red shale. This is probably not the base of the red rocks but it is certain that the base is several miles above the Erie railroad bridge where the base of the Catskill formation _ is represented as crossing the river on the Geologic map of New York and it has been so indicated on the accompanying map. 3) es NEW YORK STATE MUSEUM CONCLUSION In the conclusion of part 1 of this report some general results were stated, but itis now thought best to summarize very briefly ae | all the important results of this investigation. oe 7 1 It was shown that from Cortland county east across Che- Tis nango, Otsego and Schoharie counties the line marking the upper boundary of the Hamilton formation is from 5 to 15 miles farther north? than it was drawn on the Preliminary geologic map of New ge York. = | 2 The Tully limestone extends eastward to Smyrna in the Che- 1s nango valley and of course for that distance clearly indicates the top of the Hamilton formation. Above the limestone at Smyrna is the Genesee slate nearly 30 feet. thick which was not — .clearly recognized to the east of the Chenango river. 3 The horizon of the Tuily limestone is indicated in New Lis- * bon township in the southern part of Otsego county by the occur- rence of its characteristic fossil Rhynchonella (Hypothyris) venus- — tula Hall. This discovery extends the distribution of the species 30 miles farther southeast than heretofore reported. ee 4 Succeeding the Tully limestone and Genesee slate, or farther east where these formations have disappeared, the Hamilton formation, is a mass of thin bluish sandstones and smooth shales of Portage age, for which Vanuxem proposed the name “ Sher- burne fiagstone ” which has been adopted and used as the name for the formation. It has a thickness of 250 feet in the Chenango valley and may be readily traced westward to the meridian of — Cayuga lake, west of which Prof. J. M. Clarke has shown that it gradually passes into the Naples beds. Eastward from the Che- nango valley the Sherburne formation crosses Chenango, Otsegoand Schoharie counties, entering Albany co. where it turns south- 2 southwesterly, and apparently extends to the Delaware -river crossing Greene, Ulster, Sullivan and Orange counties. Where the Sherburne formation is separated from the Hamilton by the a By a typographical error on p. 220 of part 1 of this report the writer was made to say south in- > stead of north, but from the numerous statements in the descriptive portion of the paper concerning “aes this boundary the mistake would be apparent to one specially interested. Plate 26 NKOOPHALLENBEC GEE Ss HAMILTON. SAWKILL FALLS, MILFORD, PA. a wees ee mee re a CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 313 — Tully limestone and Genesee slate, fossils are comparatively rare in it, but to the east of the Chenango valley in Otsego and Scho- - harie counties they are more common and constitute a modified Hamilton fauna. In eastern New York across Greene and Ulster counties the upper part of the flagstones or ‘ North river blue stone” is apparently in the Sherburne formation, but contains scarcely any fossils except occasionally a few species of plants. 5 Above the Sherburne is the Ithaca formation which has a thickness of 500 feet in the Chenango valley and extends from the vicinity of Keuka lake where it has been shown by Prof. Clarke that the “ Portage or Naples fauna prevails largely to the exclusion of representatives of the Ithaca fauna”® eastward across Schuyler, Tompkins, Cortland, Chenango, Otsego and Scho- _harie counties. In eastern New York across Albany, Greene, ‘Ulster and Sullivan counties the physical conditions which ex- isted during the deposition of the Oneonta and Catskill forma- tions appear to have also prevailed during Ithaca time and per- haps they began in the Sherburne, so that there is very little evidence of the Ithaca fauna, the fossiliferous, bluish and grayish shales of the more western counties being replaced by the unfos- siliferous red and greenish shales and sandstones. In Orange county and northeastern Pennsylvania there is some representa- tion of the Ithaca fauna, the reds appearing later as one follows this series to the southwest. Prof. Clarke has clearly shown > that the Ithaca fauna in the Chenango valley is cemposed of “a more abundant representation of unmodified Hamilton species ” than in the Ithaca region,? which is also true to the east of the Chenango valley as demonstrated by the numerous lists of fossils given in this report. . 6 From the Chenango valley eastward the Ithaca is capped by the Oneonta formation which is composed of red and green shales, reddish sandstones and coarse grained grayish to greenish gray sandstones. These rocks are nearly unfossiliferous, con- taining only an occasional specimen of Archaeopteris and Amni- age group.” b Ibid. p. 46-63. o14 NEW YORK MUSEUM | STATE genia catskillensis (Van.) Hall. The formation has a thickness Of —- 550 feet in the Chenango valley and as the physical conditions _ under which the Oneonta was deposited appeared earlier to ages - eastward it gradually thickens in that direction till in Albany ae and Greene counties it completely replaces the Ithaca formation. , f 7 The Chemung formation east of the Susquehanna river rapid- ly thins to the eastward on account of the earlier appearance of ‘ the physical conditions which prevailed during the deposition Of. the Catskill formation, so that the lithologic characters of the —__ Chemung are gradually replaced by those of the Catskill, and — an are es as this change takes place the Chemung fauna disappears till the — a farthest east it was noted was near Spring lake northwest of - & Delhi where a small Chemung faunule occurs above red shales. Search in the rocks occurring at the horizon of the Chemung formation east of the Delaware river was not rewarded with any : fossils and the lithologic appearance of these rocks is similar to that of those composing the Oneonta and Catskill formations. poe 8 In eastern New York in Albany, Greene, Ulster and Sullivan counties the physical conditions under which the Oneonta and 7 Catskill formations were deposited began.as early as Sherburne - : time and continued throughout the remainder of the Devonian period. The representation of the Ithaca or Chemung faunas is very slight and this great mass of rocks consists mainly of alter- nations of red and green shales and sandstones and gray to green- ish gray, coarse grained sandstones with some conglomerates in the Catskill mountains. In the Delaware valley the red rocks do not appear as early and there is some representation of the Ithaca fauna which is more pronounced in northeastern Pennsyl- vania. As this series of rocks is followed along the Appalach- ians southwesterly across Pennsylvania, Maryland and the Vir- ginias it is found that the reds gradually appear later and the Chemung fauna is present. For in western Maryland, succeed- — ing the black shales with a Genesee fauna at the top of the Ham-- : ilton, are first nearly barren smooth shales and sandstones like 2 the Portage of western New York, then rougher shales and rather 2 mealy sandstones containing an abundant Chemung fauna with CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 315 numerous specimens of Spirifer disjunctus in Garrett county and finally the red and grayish shales and sandstones of the Catskill. This change from the Catskill mountain region to the southwest is found to be quite similar in general characters to the change from these mountains westward across southern New York, the story of which was excellently told some years ago by Prof. Stevenson in his address before the American association for the advancement of science.? . Correction. On the “ Geologic map of parts of Chenango, Madi- son, Otsego, Schoharie, and Albany counties ” accompanying part 1 of this report, published in the 15th annual report, the southern margin of the colored area is not intended to represent the bound- ary either of the Chemung or Oneonta formation. The engraver has made the line a regular one as though it represented a bound- ary, while it was intended to have been an irregular, broken one — which would have shown clearly that it is not to be considered the southern boundary of those formations. a The Chemung and Catskill (upper Devonian) on the eastern side of the Appalachian basin. Proc. — American ass’n adv. science, 1892, 40:219-48. Appendix Upper Devonian fish-fauna of Delaware county, New York By ©. R. EASTMAN The following notes are based on a small collection of fossil fishes from the base of the Catskill formation in Delaware county, New York, together with a few specimens from the Che- mung group near Franklin Station in the same county and one or two other localities, which were collected by Prof. Charles 8. Prosser during the prosecution of his geologic survey of this -region, and were turned over by him to the writer for examina- tion and report. | _ The material may be said to be fairly representative, and though its state of preservation is not so favorable as one might desire, yet it is fully as good as the average that can be obtained from rocks of this age in New York state. Most of the specimens show signs of having been drifted about by currents prior to de- position. The plates of Bothriolepis, for instance, are invariably found detached, and their ornament more or less abraded. But though the heavier fragments have suffered severely, delicate objects like the scales of crossopterygians sometimes occur almost wholly uninjured. The latter probably became detached and covered with sediment very close to the spot where the dead creature finally sank to the bottom. Although our knowledge of the higher Devonian fish-fauna in the eastern states is based for the most part on incomplete specimens, there is reason to expect it will become greatly aug- mented in the course of time, since the variety of fragments already discovered indicates a considerable diversity even as early as the Lower Devonian. It is impossible not to derive some information from the comparison of large numbers of dissociated parts; and among the latter there is always the chance of some Ao 5 laa NEW YORK STATE - exceptionally perfect specimen turning up at any moment, which | - Species, specially of free-swimming chordates, should be ob- plates and their coarsely tuberculate style of ornamentation. mee MUSEUM may afford the key to unsolved problems. The commonly de- — spised “ fish-fragments ” are therefore entitled to greater respect than most collectors have allowed, and by all means should find = = their way into repositories where they may be preserved and : a freely consulted. : ee = The chief interest of the present collection centers in its assort- _ Bes ment of Bothriolepis remains, the appendages and various plates 5 2 of the dermal armor being illustrated by more than a score of ‘ “ specimens. The species B. minor was originally described from Chemung rocks, and has not been heretofore reported from the s as Catskill formation. The occurrence of a Catskill dinichthyid oe and a spine of Onchus, as well as scales of Holoptychius amert- canus in the Ithaca group are likewise matters of general inter- est. The principal “fish-bed” of the Upper Devonian in New- York and Pennsylvania has been referred by most writers to the _base of the Catskill, though some have placed the line of demar- | “te cation higher up, owing to the persistence of typical Chemung ae * fossils. At all events it lies near the upper limit of the Chemung Pe ) formation, and in view of the general migration of forms during these epochs, it is not surprising that some intermingling of served. The New York localities, however, yield a considerably smaller number of species than those in the northern tier of 7 counties in Pennsylvania. pipe a a | Oat. z FISH-FAUNA OF THE ITHACA AND CHEMUNG FORMA- TIONS 7. ane yey he Family Coccosteidae | _ ‘ a Genus DINICHTHYS es The only species of Dinichthys hitherto described from the a - 7 ne Rye Chemung is D. tuberculatus Newb., founded on detached fragments from Warren, Pennsylvania (type in Yale museum). This species ~ is remarkable for the relatively great thickness of its dermal girs dhe cre Ys i Fragments that are indistinguishable from those found at the _ CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 319 typical locality occur in the Corniferous of Ohio, Hamilton of _ Milwaukee, and Upper Devonian of Johnson co., Iowa. _ Newberry® describes but does not figure a small dorso-median plate referred to D. tuberculatus of which the anterior half only _ was preserved. He noticed “a strong keel on the under sur- face,” but though warranted in assuming that the latter “ ter- _ tminated behind in a neck-like process projecting downward,” it iS apparent from his own statement that the latter was not observed. Had Newberry possessed other and more perfect ex- amples of this plate, he could not have failed to notice their re- semblance to his D. precursor, from the Corniferous of Ohio. A comparison of the type of the latter “species ” with several other homologous plates from the Chemung of Warren, Pennsylvania, - now preserved in the museums of Columbia and Yale universi- ties, leads the writer to believe that D. precursor and D.iuberculatus are identical, in which case the latter name takes precedence. Lest the objection be raised that the Chemung plates exhibit a somewhat different outline anteriorly from Newberry’s figure of D. precursor, the fact must not be overlooked that the latter is not strictly accurate. Newberry® states that “the keel of the under side is buried in the rock, and its form can not be made out.” The truth is that the keel, which lay uppermost and was exposed, has been almost entirely broken away; and the dorsal side of the plate is embedded in the rock, or where abraded or corroded away, has left its impression in the rock. lateral ee sometimes ornamented but in ers cases: ae the antedorso- median, thus Adtenianes that all are the produtl of = the same cause, and are correlated with the condition of overlap. — The collection also contains two pectoral appendages belonging < oa a to the left side of the body, one of them being preserved in coun- — terpart. They are about the average size of those in B. bee i Some of the ventral plates likewise indicate less disparity in size of the two species than has commonly been supposed. No exam- i ples of the head portion are represented in the collection. = - : Locality; same as preceding. ‘ oe ae, Family Coccosteidae Genus DINICHTHYS * ae Dinichthys sp. | ae The dinichthyid plate of which the visceral aspect is shown in the annexed figure is identifiable as the left anteventro-— iS lateral. It is nearly entire, lacking only — =e -a small piece from each of the antelateral mae angles. In length it measures 4.4 cm, and ~ a in maximum breadth 2.8 cm. It is quite thin, and this circumstance taken together — é ae with its outline and rugose markings one 5 | the posterior and inner margins, due prob- % = ably to overlap, compel us to refer to it to bts : ‘the ventral surface of the body. There is an obvious similarity in outline to the cor: =a responding plate in D. minor,“ and a lesser Fig. 6. Dinichthys sp. Visceral surface of right anteventro- sides ha dae teus. As the external surface is firmly em- = bedded in the matrix, it is impossible to observe the nature of — the ornamentation, and hence a specific determination is quite _ resemblance to the same element in Coccos- a Cf. Newberry, J. S., loc. cit. (1889). pl. 47, fig. 2. CLASSIFICATION, ETC. OF HAMILTON AND CHEMUNG SERIES 327 impossible. In point of size, however, it would correspond to a young individual of D. tuberculatus from the Chemung. No species of Dinichthys has yet been described from the Catskill, and it is therefore to be hoped that further material of this nature may be forthcoming. i Locality ; Kaaterskill creek above Palenville. Family Holoptychidae Genus HOLOPTYCHIUS H, oloptychius americanus Leidy Scales of this species are quite abundant in the Catskills, and were obtained in considerable numbers from the same locality as Onchus and Bothriolepis, i. e. from the Ontario and Western railroad tunnel between Murickville and North Walton, in Dela- ware co. Associated with the above were several specimens illustrative _of the scales and bone-fragments of some unknown fish, probably of crossopterygian nature. The scales are about 2 cm in diame- ter, and somewhat elliptic in outline. The external surface is. smooth without being either polished or enameled, and under a lens is seen to be covered with innumerable minute conical eran- ules. The latter are hollow, and consequently appear as pores on abraded or fractured specimens. The thickness of the scales varies between 1 and 1.5 mm, and the under surface of some bears a prominent articulating ridge. The generic and even _ family position of these objects must be regarded for the present as indeterminable. Locality ; same as preceding. yi ‘ anaes? em has STRATIGRAPHIC GEOLOGY OF THE EASTERN HELDERBERGS BY CHARLES S. PRossER AND RicHarp B. Rows ‘Introduction : e Res ee | ee eet man hill. = een Section of Countryman hills: a ee coronas ee ‘Section. south of New Salem. . Bio aegere ss : ese 3 oe ue = a ae rape Saree 2 Scare = base bas ~ Clarksville and Oniskethau creek. . ss Seeks oom 2 nies . Clarksville and Oni kethau creek section. . 2 c os Paleontology . Winhorests nie oe ee oe ‘ s eS m e J ” a A x « t 3 2 F # ¥ ~ . - - es INTRODUCTION - The eastern escarpment of the Helderberg plateau, generally termed the Helderberg mountains, forms one of the most striking topographic features of central eastern New York. The most prominent portion of this escarpment is in the central part of Albany co. in New Scotland township where it turns from a | southerly to a westerly direction. To the south of New Scotland the Helderberg and Catskill mountains form for many miles the _ western boundary of the Hudson river valley, while to the west no less than 10 different geological formations are exposed in the of New Salem the escarpment forms the northern boundary of the great plateau region of southern New York which has re- cently been well termed by Prof. Tarr the New York-Pennsyl- vania plateau province.“ An excellent view of the most rugged part of the Helderberg mountains is offered every traveler on the ~ N. Y. C. & H. R. railroad on leaving Albany who on looking out of the car window toward the west will see a steep mountain ridge rising from 1000 to 1300 feet above the general level of the Hudson river valley. Not only is the region famous for its natural scenery but the massive limestones which form cliffs from 50 to 100 feet in hight are familiar by name at least to ~ every geologist as the Helderberg limestones. Prof. James Hall has made numerous trips to this region and the Schoharie valley and has added some hundreds to the known species of fossils so that the locality has become a classic one. Indeed, the great ‘English geologist Lyell is reported to have said after visiting the Helderberg region that no one could consider himself a per- fectly trained geologist until he had seen the Helderberg moun- tains, and it is well known as a favorite locality of Louis Agassiz for geological study. However when the writer came to study the geology of this extremely interesting region he found that no one had published a precise geological section of the northern Helderbergs. Since — aBull. Am. geog. socs 1896. 28:106, eo en: YW abe SPBo2 NEW YORK STATE MUSEUM eastern Helderberg escarpment and since it would be difficult to find a locality in New York at which the stratigraphic position of a similar thickness of rocks is as clearly shown, and finally since it is the typical locality for the Lower Helderberg series it — ‘ : seems important that the thickness, lithologic and faunal charac- teristics of typical sections of the northern Helderbergs should be published. Mather in 1843 in using the name “ Helderberg division” for the rocks forming the northern end of the Helder- berg mountains, stated that ‘in consequence of these rocks being so well developed on the Helderberg mountains, and their forming a natural group, strongly marked in their lithological — and paleontological characters from the strata lying above and below them, the term of Helderberg division is used to designate : them.’”¢ - This division included all the formations found in the northern Helderbergs from the top of the Hudson to the base of the Marcellus shale. Mather’s classification has not been gener- ally adopted but the name Helderberg is perpetuated in geolog- ical classification by the Lower Helderberg period or series. The general geology of the Helderberg region has been more or less fully described by various geologists. The first work de- . scribing to any extent the geology of Albany co. is that by Eaton and Beck in 1820.6 At least a third of the work is devoted to a discussion of the different varieties of soil and their treat- ment and naturally enough the geological portion is very crude. “A section of the Helderberg” is given on p. 55 which was ap- — parently made farther north than Countryman hill. At the base — is a “compact limestone consisting of organic relics.” This state- ment is clearly an error as no limestone occurs in such strati- graphical position near the northern part‘of the mountains. Next is what is called a “ water limestone destitute of organic relics ” capped by a layer of “iron pyrites ” which is evidently the water- lime. Above this is a “ slaty sandlime destitute of organic relics ” which apparently refers to the Tentaculite limestone, while the aGeol. of N. Y. pt 1, p. 325. UGeol, surv, of the co. of Albany, p. 56. STRATIGRAPHIC GEOLOGY OF THE EASTERN HELDERBERGS - 333 Pentamerus, Shaly and Becraft limestones were apparently over- looked since the succeeding and highest division is described as a “porous sandstone containing organic relics” which judging from the statement that “ the best locality of this rock is in the town of Berne on the height of the Helderberg ”@ ig undoubtedly. the Oriskany sandstone. Next in order is the report of Mather in 1848 describing the. geology of the first geological district of New York,®? while Em- mons in 1846 added materially to the knowledge of the geology: of that region.¢ ; In 1859 Prof. Hall enumerated the formations “ comprising the Helderberg mountains proper in Albany county” and proposed the names ‘“ Lower Helderberg group” composed of the Tentacu- lite, Pentamerus, Delthyris shaly, Encrinal and Upper Pentam- erus limestones and ‘Upper Helderberg group” composed of the Schoharie grit, Onondaga .and Corniferous limestones.“ It was stated that “the Lower Helderberg group...has been so- termed from its very complete development along the base of the Helderberg mountains; constituting in this part of New York an important fossiliferous group.°® In geological classification the Upper Helderberg has been partly superseded by the term Corniferous period and series but the name Lower Helderberg series or Helderberg limestones is. still generally in use. Mr Darton has discussed recently “the relations of the Helder-_ _berg limestones and associated formations in eastern New York ” and described the geology of Albany co., adding considerably to the knowledge of the stratigraphical and structural geology of the Helderbergs. However on account of the absence of any detailed section in the above works the authors of the present paper decided to describe two typical sections of the eastern flank 7 a Geol. surv. of the co. of Albany, p. 29. A description of the geological divisions men= tioned above is given on p. 26-30. bGeol. of N. Y. pt 1, p. 317-53. cAgriculture of N, Y. 1:153-86. dGeol. surv. N. Y. Paleontology, vol. 3, pt 1, p. 97. elbid, p. 33. See also p. 33-45. 7i8th An. rept. N. Y. state geol. 1894. 1:197-261. © 5334 | NEW YORK STATE MUSEUM — of the Helderbergs in New Scotland township, the first, Countey. oo man hill from near the nor:hern end of the Hel derbergs to the west — -of New Salem, and the second, a few miles farther south along — Oniskethau creek and in the vicinity of Clarksville. The more : northerly of the two.sections will be described first. ie NEW SALEM AND COUNTRYMAN HILL New Salem is a small village with less than 200 people located in the northern central part of New Scotland township at the foot of the steepest part of the Helderbergs and three miles south- west of Voorheesville, a station on both the Susquehanna di- ~vision of the Delaware and Hudson and the West Shore railroads. To the west of New Salem, its base being only a short distance from the village, is the rugged slope of Countryman hill which forms the highest and most precipitous point of the Helderberg range. For two miles and a quarter to the north the lower part _-of the escarpment is specially marked, being composed of massive ~ limestone cliffs which form perpendicular walls from 50 to 100 — feet high and then it turns sharply to the west. New Salem is ~ a little over 400 feet above sea level, the foot of the cliffs of ‘Countryman hill 500 feet and its top about 1650 feet A. T. The eastern side of the hill consists of three steep cliffs which are sep- arated by two marked terraces. The two lower cliffs are com- | posed mainly of massive limestones between which is a. terrace of shaly limestone and shale the central part of which is broken . by a heavy ledge of limestone and sandstone, while the upper cliff is composed principally of shales which become arenaceous to- ward the top. On top of the hill it is comparatively level for sev- eral acres while to the west is a small valley formed by a branch ~ -of the Oniskethau creek, on the western side of which rises a higher ridge which forms the culminating part of the Helder- bergs, its summit being given by the U. S. coast survey as 1823 feet A. T. From the top of these hills on a clear day a magniii- cent view of the great Hudson valley and the mountains to the ‘east may be had, a view that well repays one for the steep ascent. Plate 1 Section of Countruman Hill, New Salem. i > Marcellus &Hamilt A® Pentamerus 50! A? Fermtacotte transition tt A* Tentacu liters Se Gey Seer A’ Hudson River Covered 300’ Sea Level 3 Scale 1’=150' STRATIGRAPHIC GEOLOGY OF THE EASTERN HELDERBERGS | 33D About New Salem and part way up the lower cliff of Country- man hill the geological formation is the Hudson river which in general underlies all of the great plain from the Helderbergs east to the Hudson and north to the Mohawk river. The underlying rocks however for considerable areas of this plain are covered by - Jater formations belonging both to the Glacial and Champlain. “The Hudson river rocks about the foot of the Helderbergs consist of alternations of shales and sandstones that are comparatively barren in fossil remains. The only fossils:reported from the Hud- gon river rocks of this region, so far as known to the writer, are _ Orthis testudinaria and Trinucleus concentricus which were found by Mr Walcott at the Indian Ladder on the northern escarpment of the Helderbergs about two and one half miles northwest of New Salem.2 The formation has a great thickness in this region as shown by a well drilled near Altamont (formerly Knowersville) _ which started 595 feet below the base of Tentaculite limestone and reached the top of the Trenton limestone at a depth of 2880 feet, giving a thickness of 3475 feet for the Hudson and Utica formations to which with the exception perhaps of a few feet at the top, all the rocks in this section between the Tentaculite and Trenton limestones belong.® SECTION OF COUNTRYMAN HILL - eXXXIX A. The following section begins at the foot of the steep cliff a little north of west of New Salem and continues to the top of the hill. Feet A® Top of Countryman hill composed of rather aren- 425=1247 aceous shales that contain very few fossils. On the top are loose glacial boulders of Corniferous limestone. Near the base of this upper ridge are fine, argillaceous shales of the Marcellus shown in small draws, but the greater part of the slope is covered by soil so that it is impossible to determine aBull. geol. soc. Am, 1890. 1:345. bAshburner. Trans. Am, inst. min. eng. 1888. 16:951-53. -cUnion college geological survey. 336 . A NEW YORK STATE MUSEUM the line of division between the Marcellus and Hamilton formations. Again in the Helderberg region there is a gradual change in the lithologie characters from the Marcellus to the Hamilton, and the Marcellus shales have a ereater thickness: than in central.and western New York. It is prob- able that the upper part of the hill belongs in the Hamilton formation. To the southwest across one of the head branches of the Oniskethau creek is the highest ridge of the Helderbergs which is _ composed of slightly arenaceous shales contain- ing abundant Hamilton fossils. Cliff of massive limestone, the top of which forms the upper terrace due to the erosion of the Marcel- lus shale. The rock is light gray in color, contains in places a considerable amount of chert and is not very fossiliferous, most of the species being corals. Onondaga limestone. An impure, dark gray limestone which weathers to _ a buff, porous sandrock, shown in places at the A A’ base of the Onondaga limestone on the cliff south of west of the house of Mr K. P. Parrish, where a thickness of 2’ 10” was measured. Schoharie grit. Blackish, somewhat arenaceous shales which con- tain specimens of Spirophyton cauda-galli (Van.) Hall. Hsopus shale or Cauda-galli grit. - Very dark gray quartzitic sandstone which weath- ers to a brownish color and contains abundant fos- sils. The upper surface of this sandstone is gener- ally covered with markings of Spirophyton cauda- gall, and it forms the upper part of the lower ter- race. Oriskany sandstone. Ledge of massive, light gray, fossiliferous limestone which is well exposed for some distance above the highway in the vicinity of the house of Mr K. P. 100-822 3-723 121-719 | “O=598 | 13-596 — Plate 2 *._” WYNKOOP HALLENBECK CRAWFORD CO BOULDER OF CORNIFEROUS LIMESTONE; TOP OF COUNTRYMAN HILL ; & < Sa ph at » 2 et .. Shion € A® Parrish. This limestone was formerly called the Upper Pentamerus but recently Prof. Hall has named it the Beeraft limestone.? Grayish calcareous shales and shaly limestones. The shales contain great numbers of fossils many of which are nicely preserved. This formation con- stitutes the lower part of the first terrace to the west of New Salem and has the most gentle slope of any of the formations composing this part of the hill until the talus at its base is reached. Shaly limestone. : Massive bluish gray limestone forming the upper part of the conspicuous cliff to the west of New Salem. This limestone forms the upper part of the prominent cliff which may be followed from south- west of New Salem around the northeastern and northern ends of the Helderbergs to Altamont. An excellent idea of themassive appearance of thislime- stone is given in an accompanying plate the upper part of which shows the limestone as it appears on the western side of the “Indian Ladder” road at the northern end of the Helderbergs. Pentamerus lime- stone. Thinner bedded limestones than the above which are transitional in lithologic and faunal characters from the Pentamerus to the Tentaculite limestone. Dark blue thin-bedded limestones, the layers of which are generally from one to three inches in thickness and break with a ringing sound. These thin limestones form the lower part of the vertical cliff from New Salem around the northern end of the Helderbergs to Altamont. Tentaculite lime- stone. a@i3th an, rep’t N. Y. state geologist, p. 212. STRATIGRAPHIG GEOLOGY OF THE EASTERN HELDERBERGS | 337 Feet 120-583 50-463 12-413 34-401 | 338 ae yA? NEW YORK STATE MUSEUM Covered by soil and talus. Bluish eray, fairly massive sandstones which alter- nate with dark colored argillaceous shales. Hudson rier sandstones. Covered by soil, drift and talus to the foot of the Hala’ SECTION SOUTH OF NEW SALEM = ) 300=300 In the above section the contact of the Hudson formation and the overlying limestones is covered, but in a small glen west of the house of Rensselaer Markel one half mile south of New Salem the contact is clearly shown. The section of this glen is as follows: Bp’ B B Massive limestone forming cliff at the head of the run which is the southerly continuation of the lower cliff directly west of New Salem. Pentamerus lime- stone not giving however the entire thickness of the formation. . : Transitional layersfrom the Pentamerus to the Ten- taculite limestone, containing Spirifer vanuxemi Hall and Leperditia alta (Con.) Hall. Thin bedded dark blue limestone. Tentaculite limestone. Drab, impure limestone, well exposed in the run at the foot of the cliff. These beds are shown in the accompanying plate. Waterlime. Greenish sandstone to coarse arenaceous shale con- taining plenty of iron pyrites, 10 inches in thick- ness. Possibly it represents the attenuated Clinton formation. Dark blue to olive tinted argillaceous shales well ex- posed in the steep banks of the brook. Hudson rwer _ shales. a Given at 6’’ instead of 10’’ for convenience in summation of section. Feet 38-180 124-149, 90-90 os he * ta ho \ PER ee a : eae eS ee ee ee a Us JOMMeY JAMO] “UOJULTO ‘fo}l[NoVJUST, puv OUT]IOIVM UdOMJoq OUT] SuTyaeuUT sjuopnis szsddQ WHTVS MAN “ANOLSAWIT ALITINOVING, GNV ANIIUOLVA " wr % ‘ as ei id eg ny VA AS a a AEs aun 1 ree? he SMM che ie akties a ; ~ ee tah » o i STRATIGRAPHIC GEOLOGY OF THE EASTERN HELDERBERGS 339. PALEONTOLOGY The data for the preparation of this article have been obtained while directing the work of the ciass of Union college in field geology and there has not been the opportunity for a thorough collection of the fossils from the different formations. Tentaculite limestone. This limestone contains but a compara- tively small number of species, and only three that occur fre- quently. Of these Tentaculites gyracanthus (Eaton) Hall is so abundant as to suggest the name for the formation. The follow- ing species were obtained: 1 Tentaculites gyracanthus (Eaton) Hall (aa) ‘ 2 Spirifer vanuxemi Hall (aa) 3 Leperditia alta (Con.) Hall — (aa) { Megambonia aviculoidea Hall (r) 5S Modiolopsis (?) dubia Hall RT) 6 Chaetetes (Monotrypella) arbusculus Hall (r) Pentamerus limestone. This limestone like the Tentaculite con- tains but a small number of species. The Pentamerus galeatus Dal., or Sieberella galeata as it is now called by Professors Hall and Clarke is fairly abundant and furnished the name for the formation. Below is the list of species collected: 1 Sieberella galeata (Dal.) H. & C.=Pentamerus galeatus Dal. (a) 2 Uncinulus mutabilis (Hall) H. & C. 3 Atrypa reticularis (Linn.) Dal. Shaly limestone. This contains a larger number of species than any other formation exposed on Countryman hill and on account of the softer nature of the rocks of which it is composed, it is not so generally exposed as the other limestones of the Helderberg mountains. One of the best localities for collecting yet seen in the northern Helderberg region and the one that furnished the following species is along the highway below the house of Mr Kk. P. Parrish: 1 Stropheodonta (Leptostrophia) becki Hall (Cc) 2 Spirifer perlamellosus Hall (a) 3 Leptaena rhomboidalis (Wilckens) H. & C. (a) 340 NEW YORK STATE MUSEUM 4 Trematospira globesa Hall , - (e) 5 Spirifer cyclopterus Hall -(e) 6 S. macropleurus (Con.) Hall (c) 7 Stenoschisma formosa (Hall) H. & C.=Rhynchonella formosa H. (r) 8 Atrypa reticularis (Linn.) Dal. (r) 9 Meristella arcuata Hall (r) 10 Orthis (Dalmanella) planoconvexa (Hall) H. & C. 2 11 Nucleospira ventricosa Hall . (r) 12 Strophonella punctilifera (Con.) H. & C. (c) Some of these specimens seem to be the species called S. cavumbona H.; but it is said to be identical with S. punctilifera (Con.) H. & C. in Paleontology, vol. 8, pt 1, D.. 208. 13 Tentaculites elongatus Hall ~ (r) 14 Streptelasma strictum Hall (r) 15 Fenestella sp. : (c) ‘16 Dalamanites pleuroptyx (Green) Hall (r) 17 Crinoid segments | 18 Uncinulus vellicatus (Hall) H. & C Shynohonen vellicata Hall (r) 19 Lichenalia torta Hall (r) 20 Uncinulus abruptus (Hall) H. & C. = Rh yienOneMn abrupta A tall | (r) 21 Favosites sphaericus Hall (r) 22 Hatonia medialis (Van.) Hall . (r) 23 Rhynchonella transversa Hall (?) , (r) 24 Orthoceras sp. 25 Trematospira multistriata Hall (r) 26 Avicula tenuilamellata Hall (?) (r) Becraft limestone. This limestone was formerly called the Up- per Pentamerus on account of the abundance of Pentamerus pseu- dogaleatus Hall—now called Sieberella pseudogaleata by Hall and Clarke—but in 1894 Prof. Hall gave it the name Becraft lime- stone from its occurrence on Becraft mountain near the city of ee td - Plate 4 BECRAFT LIMESTONE AT NEW SALEM ae acer Wi TOS Cpe elie RS. ac FeAl en tr hag ae 3 09, 7 cer tae { > ee a PE ge : eo le ature rN Ve 7 74 Got Th ot he wv . ’ ‘ ™: iy } Le Aaa % _ , > ; Peatied sake, cae ae a + . 2 r Roane eal Bi "4 : : rs “s a 4 * . = ~~ STRATIGRAPHIC GEOLOGY OF THE EASTERN HELDERBERGS 341 ‘Hudson, Columbia co. This limestone forms a conspicuous ledge near the house of Mr Parrish, the top of the shaly limestone being shown in the spring below the house. The top of the . limestone is bare for some distance and numerous joints are nicely shown. This is a gocd locality for collecting and the following list was obtained in that vicinity: 1 Spirifer concinnus Hall — (a) 2 Sieberella pseudogaleata (Hall) H. & C.=Pentamerus pseu- dogaleatus Hall (a) 3 Atrypa reticularis (Linn.) Dal. ; (a) : 4 Wilsonia ventricosa (Hall) H. & C=Rhynchonella ventri- - cose Wall): : (r) 0 Rhynchonella (Uncinulus) nobilis Hall (c) Gh. (U. ) campbellana Hall (r) 7 Orthis (Schizophoria) multistriata Hall (c) ee 0} (Rhipidomelia) oblata Hall (r) 9 Spirifer cyclopterus Hall (?) (r) 10 Leptaena rhomboidalis (Wilckens) H. & C., (r) 11 Orthothetes cf. woolworthana (Hall) H. & C. (r) 12 Aspidiocrinus scutelliformis Hall . (a) 13 Lichenalia torta Hall (r) 14 Streptelasma strictum Hall sae ae (r) (15 Favosites sphaericus Hall Cr) 7 16 Bryozoa sp. Oriskany sandstone. This sandstone is well exposed back of Mr Parrish’s house where it rests directly on top of the massive Becraft limestone. The section differs in this respect from those on West mountain west of Schoharie where an. upper shaly lime- stone occurs between the Becraft limestone and. Oriskany sand- stone. The Oriskany sandstone on Countryman hill is very fos- siliferous, the following species having been collected from the ledge just west of the Parrish house: 1 Spirifer arenosus (Con.) Hall (a) Ze Se, arrectus Hall (a) 38 pyxidatus Hall (ye a13th an. rep’t N. Y. state geologist, p. 212: 342 - NEW YORK STATE MUSEUM 4 Rensslaeria ovoides (Eaton) Hall 5 Hatonia peculiaris (Con.) Hall 6 Merisiella lata Hall 7 Leptocoelia flabellites (Con.) Hall 8 Orthis (Rhipidomella) musculosa Hall “9 Hipparionyx proximus (Van.) H. & C. (?) Small specimens, probably young individuals 10 Platyostoma ventricosa Con. | (r) : 11 Orbiculoidea-ampla (Hall)—=Disema grandis (Hall) H. & Cy (yee ‘12 Orthis sp. (Eee 13 Stropheodonta cf. magniventra Hall (Tey 14 Platyceras nodosum Con. (r) CG. 8. P. CLARKSVILLE AND ONISKETHAU CREEK Clarksville lies about 12 miles southwest of Albany on the Delaware turnpike in the southwestern part of New Scotland township. The village is in a small depression with Bennett hill on the south and Wolf hill on the west, while on the east and. north is a ridge from 50 to 100 feet high. There is little doubt that this depression was at one time a lake. Oniskethau creek however long ago cut a gorge 100 feet or more el through the ridge to the east. The Oniskethau creek rises in the Helderberg mountains west — of Wolf and Countryman hills, and flowing east between them turns southeast along the base of Wolf hill and passing through the villages of Clarksville and South Bethlehem unites with the Spraytkill to form Coeymans creek which enters the Hudson at Coeymans. At Clarksville the Oniskethau breaks through the Upper Helderberg formations making two deep and narrow gorges; one 75 or more feet deep through the Onondaga limestone just above the village, and the other which has just been men- tioned through the ridge of Esopus shales east of the village. About two miles southeast of Clarksville at the saw mill of Cornelius Slingerland a less conspicuous cut is made through the shaly member of the Lower Helderberg series. At the head Plate 5 Limestone Onondaga Schoharie FA ae . a | Esopus shale _—_————_______. 50. Scale Overthrust & Folds near Clarksville. STRATIGRAPHIC GEOLOGY OF THE EASTERN HELDERBERGS 343 of this cut is a fall of about 20 feet, an unusual feature in the shaly formation. The gorge is fully a quarter of a mile long and is the finest exposure of the shaly that the writer has ever seen. There is a gorge through the Onondaga about 200 yards north of the one through which the Oniskethau now flows and some- what smaller than it, which the writer considers to be an ancient bed of this creek. Its situation is such that the creek might easily be turned into it now and there is no other stream in the vicinity large enough to have cut sucha gorge. At the lower end ‘of the village west of the Dutch reformed church is another evi- dence of this ancient bed. It isa little valley running north and south, the highest part of which is not more than 10 feet above the present bed of the Oniskethau, and before the gorge was cut to the east this valley must have been the outlet to the little lake which formerly existed at Clarksville. Along the base of Bennett hill immediately south of the village are seen the northernmost traces of th Ral ee ene se, Sb aa ite acer et age 1.44 SERUM RIN IR ICL op RS i ks ack ne Coke Pa Nes ie 455 92 100.37 —— ees Niagara limestone. In Schoharie co. we find the eastern end: of this formation. Its thickness is not more than five feet and it is usually a dark gray massive limestone. An exposure of it can be seen at Howe Cave just below the cement quarries of which it forms the floor. The Niagara limestone also appears in Oneida co. north of Clayville and extends westward with increasing width to the Niagara river. In Wayne co. in the town of Butler® it is a dark blue, fine grained compact limestone and is usually thin bedded. It has been : used at this point for burning lime. Other occurrences are at Rose on the head waters of Sheldon creek and in the towns of Marion and Walworth. It has been quarried at many points in Wayne co. for the manufacture of lime. ‘In Monroe co. the northern edge of the limestone passes through the towns of Penfield, Brighton, Gates, Ogden and Sweden. The outcrops at these points generally represent the beds of the upper magnesian member and its weathered surface presents a characteristic spongy appearance. | The Niagara formation presents two types of lime rock. The one a dark gray subcrystalline stone which is used for lime and building purposes, the other a gray-brown, crystalline rock with numerous cavities and containing a high percentage of magnesia. aDarton’s Helderberg limestones and associated formations in eastern New York, 13th an. rep’t N. Y. state geol. 1898, p.218. bHall. Geol. 4th dist. p.84. 4, ew _ 4, 8 adel Pa Silas Len wr. 25 . - 5 4 , - . ms t~ > 364 NEW YORK STATE MUSEUM x The area in which the Niagara limestone is found is more re- stricted than that of most of the other limestone formations of the state. The upper member of this formation is known as the Guelph limestone but is not coextensive with the lower member. It forms a lenticular bed about 20 miles long and extends from Rochester westward. In the vicinity of Rochester quarries have | been opened in it at New Brighton and Gates. As exposed in these quarries it is a grayish brown, finely crystalline limestone containing numbers of small cavities. The peculiar feature of — this rock is that it contains a large amount of magnesia and a very low silica percentage, making it very adaptable for use in the lining of bessemer converters. Helderberg limestones. These include several distinct members which are known as the Tentaculite, water lime, Pentamerus, Catskill shaly, Becraft and upper shaly limestones. The formation is a widely distributed one within the state and of considerable economic importance, containing the hydraulie limestones which are so extensively developed at Rosendale near Kingston in Ulster co. and through the western part of the state. Its members enter the state at the southeastern corner just east of Port Jervis, New York. They then follow up the southeastern side of the valley of Neversink river, Basherkill, and Rondout creek. Throughout this whole distance the limestone rests on the Shawangunk grit which forms the crest of the Shawangunk moun- tain. From Kingston the same formation extends northward past Catskill te New Baltimore where it then swings to the north- west, extending as far as New Salem in Albany co. At this point it becomes very narrow but appears again as a some- what broad belt just west of Meadowdale in the same county and then extends westward as far as Central Bridge in Schenectady co. and from there in a slightly northwest direc- tion past Sharon Springs, Dennisons Corners, Oneida, Syra- cuse, and westward to Niagara Falls. Up to Dennisons Corners the formation though of considerable thickness does not cover a very broad belt owing to the perpendicular escarpment which it forms, but its thickness remains about the same from Syracuse a Ted ae | ay? ¢ ri te Ae Lisi - ~ LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 363 westward to Buffalo,-and the elevation of the escarpment de- creases. As the Helderberg.limestones are of considerable thickness in New York state it may be well to mention them in detail. This can be best done by quoting from the report of Mr N. H. Darton.% The Helderberg limestones attain their greatest development in eastern New York, and the thickness reported by Davis of about 300 feet in the Catskill region igs the maximum. They thin gradually southward in New York, but expand again in New Jersey. In the Helderberg mountains they are 200 feet and at Schoharie not over 240 feet. Westward from Schoharie the thickness decreases very gradually. The members constituting the formation in its typical development beginning at the top are, a pure semi-crystalline, massive, very fossiliferous limestone, - a ‘thick series of shaly limestone, and the basal series, thin bedded dark limestones of the Tentaculite beds. On Catskill creek a higher member of impure shaly limestone comes in above the pure, massive beds, thickens rapidly and continues south- ward to and through New Jersey. The Helderberg formation preserves its typical characters with some local variations in thickness to a few miles west of Cherry Valley. Then the upper limestone beds thin out and on the road from West Winfield to Litchfield in the southwestern corner of Herkimer county the Pentamerus beds lie directly under the Onondaga limestone. The upper members of the Helderberg limestones which come in again westward and are finely exposed at Oriskany Falls.?_ Here 120 feet of beds are exposed in and about the quarries, of which 50 feet are quite distinctly of the Tentaculite beds, 40 feet of gray beds in greater part of Pentamerus limestone age, but merging into the character of the lower beds, a few feet of beds with mixed Pentamerus and shaly limestone fauna and at the top 25 feet of gray subcrystalline rock containing a shaly limestone fauna. 25 miles west of Perryville, Madison co. this condition has continued, the lower members expanding ap- parently at the expense of the Pentamerus beds and the upper members giving place to Pentamerus beds. At this locality the Onondaga limestone was seen lying on a few feet of dark gray limestones containing Pentamerus, with a thin local intervening layer of Oriskany at one point, which gave place to a great mass of thin bedded gray limestone below. a Report on the relations of the Helderberg limestones and associated formations in eastern New York. 13th an. rep’t N. Y. state geol. 1893, p.204. b See also S. G. Williams. The westward extension of rocks of the Lower Held- erberg age in New York, Amer. jour, sci. 3d series, 31:139-45; Abstract Am. ass, adv. sci. Proc. 34:235, 236; Amer, nat. 1886, 20:373. = ns al ae Al 366 NEW YORK STATE MUSEUM The Salina formation which is such a prominent member of | the series in central and western New York, thins rapidly east- ward and is finally represented by an attenuated development of its upper members. This representative is the waterlime series which is more or less continuous through eastern New York, northern New Jersey and Pennsylvania. In the country of the Helderberg mountains it is not always recognizable and when present is often not over a yard in thickness. About Rondout and Rosendale it comprises thick beds of valuable cement rock and at Howes Cave there is also a cement bed of workable thick- ness. The Onondaga limestone. This is the limestone series which is usually termed the ‘ Corniferous” by many writers, but by others the upper member of the series is termed “ Corniferous ” -and the lower member “Onondaga.” As both members are | cherty the term Corniferous implies a contradistinction which does not exist, and it has been proposed by Prof. Hall to revive the term “Onondaga” to comprise the entire series. It is a well-known name in western New York where the beds — are extensively quarried, and the formation is typically devel- oped in the Onondaga region. As the name Salina has been finally adopted for the salt and gypsum group of the upper Si-— lurian there need be no confusion attending the general use of “Onondaga ” for the limestone as proposed. The subdivisions of the Onondaga group gradually lose their physical and faunal characteristics in eastern New York and the formation is in greater part a bluish gray subcrystalline, mas- sive limestone with lenticular masses of chert in courses and irregularly disseminated. Darker colors occur locally, notably — in the upper beds about Peoria (West Berne) which are very dark and coarsely crystalline. The chert is predominant in the upper beds but it is usually present also in the lower beds. In places it is an inconspicuous feature but this is not often the case. Thin partings of shale occur rarely. About Saugerties the lower portion of the limestone is shaly and weathers buff. About Clarksville the lower members are very pure, free from chert and regularly bedded. ~ LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 367 - In Greene and Ulster counties particularly the outcropping edge of the formation is characterized by a fringe of very large diseonnected blocks occurring at various intervals. In some cases these klocks lie several hundred yards from the edge of the outcrop. ; Helderberg limestones. The members comprised under this name are the Upper shaly beds, the Scutella or Upper Pentam- erus beds, the Lower shaly or Catskill shaly beds, the Pentam- erus beds and the Tentaculite beds. These members preserve their distinctive characters throughout the region to which the report relates though there are occasional slight local variations. The so-called Scutella beds are the uppermost member south- ward to near Catskill. They are light colored coarsely semi- crystalline massive bedded, highly fossiliferous limestone blotched with calcite replacement of fossils, of which the most conspicuous is the so-called Scutella. These are the cups or pelvis of a crinoid, having a diameter in greater part from one to two inches, and the white calcite of which they consist contrasts strongly with the light bluish gray of the containing limestone. - In the Schoharie region where these cups characterize the lower beds of the member, the overlying layers have been called the upper Pentamerus beds from the fossil P. pseudogaleatus which they contain and this name has been employed to some extent to comprise all the beds. In the eastern extensicn of the formation the distinction is lost. About Catskill, Davis desig- nates the lower. layers the “ Encrinal ” and the upper layers the “Upper Pentamerus” limestone. Owing to the inappropriate- ness of the. name Scutella and the varying significance of the other names that have been employed, the geographic name of Becraft limestone has been suggested by Prof. Hall. The name is from Becraft mountain in Columbia co. where the rock is typically developed. The Becraft limestone has a thick- ness of 10 to 15 feet near Schoharie and the amount does not vary greatly eastward to the Helderberg mountains and by Clarksville, Aquetuck and Coxsackie. Thence it increases rapidly and Davis reports a thickness of 120 feet below Leeds, 368 NEW YORK: STATE MUSEUM the upper 10 feet consisting of impure and sandy or shaly layers. There are as Davis suggests many local slips in this section and © my estimate of the thickness of the purer limestone would be tT) about 60 feet. | “In the Rondout region the Becraft limestone is 40 feet thick and the upper shaly beds 100 to 150 feet thick. In the ridge just east of Whiteport there are 30 feet of Becraft limestone.” About Rosendale and southward no exposures have been noted by Darton. ‘“‘ Underlying the Becraft limestone throughout are the lower shaly beds consisting of thin-bedded, impure, highly fos- siliferous limestone with some shale beds.” At some localities though, as for instance westward on the Foxkill above Gallup- ville, it is in greater part a massive, relatively pure limestone. _ In Greene and Ulster counties it has the character of the upper shaly beds, with a more or less slaty cleavage and outcropping in ragged ledges, in some cases closely resembling the lighter colored outcrops of the Esopus slate. Its thickness from Scho- harie eastward is about 80 feet, and there and elsewhere in the © great Helderberg escarpment it constitutes a steep slope between the Scutella and Oriskany shelf above the Pentamerus escarp- ment below. Its thickness apparently decreases somewhat in the Kingston-Rosendale region but it retains its characteristics. The Pentamerus or lower Pentamerus are the most conspicu- ous members of the lower Helderberg formation. They give rise to the great escarpment which marks the eastern edge of the Helderberg formation as it passes along through central New York. The beds are mostly hard, massive bedded and vertical jointed limestones. The rock is generally bluish gray in color but weathering imparts a lighter tint to the surface. Partings of slate occur occasionally as well as lenses of chert, specially in the east and south. 3 The Pentamerus limestone is a quite uniform member and its thickness does not vary greatly. “At Schoharie its thickness is between 60 and 70 feet, in the Helderbergs it is the same and a trifle more about Catskill (80 feet according to Davis), 50 feet at ae LIMBSTONES OF NHW YORK AND THEIR ECONOMIO VALUB 369 Saugerties, 30 to 40 feet about Rondout, 70 to 100 feet about Rosendale, the maximum being in the ridge just northwest of the village. The Pentamerus beds are quite sharply demarked from those above and below them.” ; The finest exposures of the Pentamerus ledges are in the great escarpment of the Helderberg mountains near the Indian Ladder where they rise in great cliffs surmounting steep slopes to an altitude of 700 feet above the plain lying to the north and east. The Tentaculite beds are thin bedded dark blue limestones, lying below the Pentamerus beds, and usually constituting the base of the Pentamerus escarpment or lying beneath its talus. The beds vary in thickness from an inch to a foot in greater part _ but two or three inches is the average. The Tentaculite beds have a thickness of 40 feet at Howes Cave and Schoharie, somewhat less in the Helderberg mountains and from 30 to 40 feet through the Catskill and Kingston regions. In the Rosendale region the amount is less. ‘here are several outliers of the Helderberg limestone of which an important one is Becraft mountain. Salina waterlime. The attenuated eastern extension of the great Salina formation is of variable character and thickness and may not be continuous throughout. Locally it consists of heavy beds of cement rock but generally it is composed of thin _ beds of more or less impure cement intercalated with thin bedded limestones of varying character. The cement beds attain their greatest development around Ron. dout and Rosendale where they are extensively worked. The ce- ment rock is a blue black, very fine grained, massive bedded deposit of calcareous magnesian and argillaceous materials and is of some- what variable character and composition. The rock produces a cement of good quality only when the components bear certain relative proportions to each other. A characteristic feature of the rock is the light buff hue to which it weathers on the surface. At _ Rosendale there is a 21 foot bed of the cement at the base of the formation, then from 12 to 15 feet of mixed impure cement and limestone beds, then another cement bed 11 feet in thickness. Above these are the Tentaculite and Pentamerus. These cement beds with some variations in thickness, and many in character, extend over a wide area from north of Whiteport through Rosendale to beyond High Falls, outcrop- Uae, Ce 310 NEW YORK STATE MUSEUM — (aS are ping in a belt about eight miles long and two and a half wide. — A At High Falls there is an upper bed of cement 15 feet thick and a lower bed five feet thick separated by three feet of impure limestone. At Whiteport the upper cement bed is 12 feet thick, the lower from 15 to 20 and the intervening limestone 10 feet in thickness. How far they may extend under the overlying rocks to the westward is not known and their southern termination has not been explored. To the northeast the cement thins out rapidly and gives place: to impure cements and limestones, but it thickens again rapidly in the Rondout region. At Rondout there are two cement beds, the lower one is 22 feet thick and the upper five feet thick with three feet of limestone and cement in- tervening. Northwest the lower cement bed thins. : Origin of limestone Most limestones are of marine origin, few of them being fresh- water deposits. They result generally from the accumulation on the ocean bottom, of the calcareous remains of marine organ- isms, such as the shells of mollusks, the cases of foraminifera, Skeletons of corals, etc. These are sometimes plainly apparent in the limestone, but very often the shells become comminuted before settling on the ocean bottom, or they may be broken by the _pressure of other material deposited on them, so that not in- frequently limestones show no trace whatever of organic re- mains. Limestones of great purity have generally been. de- posited in the deeper portions of the ocean, far enough away | from the shore to prevent their contamination by siliceous or argillaceous sediments brought down to the sea by rivers. The varying intermixture of such classes of material with the cal- careous mud results in the formation of all grades of rock be- tween a limestone and sandstone on one hand, and a shale on the other. A siliceous limestone is one with siliceous impurity, which if the silica predominates is called a calcareous sand- stone. In the same way we may have a shaly or argillaceous limestone or a calcareous shale. 3 Limestone may also be formed chemically, viz, by the deposi- tion of a calcareous deposit from waters having carbonate of lime in solution. SM ep, LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 371 Composition of limestone calcitic and consists of 56% of oxid of lime and 4474 daeboute calcite and consists of 56% of oxid of lime and 44% carbonic acid. It rarely occurs perfectly pure as the impurities seldom get below 1%; they may also increase to such an extent as to prohibit calling the rock a limestone. The impurities commonly present are silica, alumina, iron, magnesia and organic matter. ’ Traces of sulfuric and phosphoric acid are also met with. The silica may be present as pure quartz or combined with the alumina in the form of clay, and less frequently as an ele- ment of silicate minerals such as mica, hornblende or pyroxene. It may practically be looked on as an inert impurity dis- placing so much carbonate of lime. At high temperatures how- ‘ever when the carbonic acid has been driven off and oxid of lime left, the silica will flux this lime with great eagerness. Alumina is usually present as clay. . With an increase in the per- centage of the latter limestone passes into cement rock. If present to the extent of 4% or 5¢ alumina is an inert im- purity like silica, but when present in larger amounts it facili- tates the expulsion of the carbonic acid gas. The reason for this is that clay contains chemically combined water which only passes off at a red heat or at the same time as the carbonic acid — gas. This provides an atmosphere of watery vapor into which the carbonic acid gas escapes quicker than it would if passing off into gas of its own kind. ; Iron and alkalies if present in appreciable quantity render the limestone more easily fusible, and may necessitate the handpick- ing of the burned rock to*separate clinkers. Magnesian limestones are known as dolomites when the per- centage of magnesia is 20 or over. The rock may have special uses, but when in smaller amounts as 2 to 124 it is to be looked on as displacing equal quantities of carbonate of lime and for certain purposes as a deleterious impurity. _ Organic matter is rarely absent in limestones and a very small * amount may impart a gray or even black color to the rock. NEW YORK STATE MUSEUM Bate! - = when only : a few Bas a “aie are used, at becomes an ‘aoe item when the consumption of a given. stone by one works is 8 200— or 350 tons a day. The former when burned falls to pieces in water with the vale = tion of heat or slakes. The latter when burned does not slake e but | forms a hard mass on the addition of water. - ee x = Uses of limestone oa: a ae Furnace flux pes s' ee This.is one of the commonest uses of limestone. It is used as Se a flux for both lead and iron ores. In the blast -furnace - the a = ae action of the limestone is to reduce the iron to its metallic state _ = and also flux the impurities which pass off as slag. 3 ie The purer the limestone the more efficient will be its action = = and the cheaper its use, for it will be easily seen that the greater . = the percentage of impurities the more limestone will be required — to do the same amount of work. | = For reasons of economy blast furnace operators often use less ee pure but more easily and cheaply obtained limestones. so8 =e ze giving the value of limestone containing varying amounts of = silica, lime and magnesia. The basis of the calculation is mag- re - nesian limestone at 56c a ton and fuel at $3.50 a ton, both at the er Some time ago a table was prepared by Mr J. M. Hartmann* e Se furnace. a Mineral resources of U. S. 1883-84, p. 670. ie Pa oe: 373 S| | | ree | 9 e003) ST | OG OT Meee Ch ale ae Gh Oe eee ay GF GT Bar. 06 =| 9 Oe pie 1s 06 YS Oh ines haa ates) Sep te OR cs ie LT OF FI a) eg | 9 Reser O tio OG uc! Oly oC eebie Rime ereGen Pisa ode x bee bet. "0G Of Tk aT la 96 | 9 pera i |G Ok OP eae veel ee wie beau, Gls i 8G ly | 8 Jha oie cae be) chek eee OP 96 kale re Shs BBO te bs Ot ee al ate & Te Se Oe ON lepers Lisi 08 MON SAO Re eC esl OSs! Ak lq he SF OT re ve | 2 1 6 2G eee. siete G 6 6g GT eg 6 0g SF 6 Bay y hea) «2 LS eee OMe TL Ol LS ARO minh 2 ener SB 8 g¢ 6F | 8 a) See eat i ag Chia Cire we ute 1 Seer aed Gy leads Sie Peale wots: OF 6F L Me ere Ch | 9 CF oR i RE RO Byes Gee eral G 68 0g 9 z, op ht cr | ¢ Pea Tee bobs me ieee OG. OLE ale eee aaa 8 Gt Oa i 9g z Shoo S Eye y OG oT hovel aie? aan OT Cah cF Tg F pee ee ake -be8 TH | & So Gh | Oy kee OO OL she OG. alae SF 6g g Ag eg | 8 Pia be Oo 2 ..GE Oye s hae Raed NO Tk OBA ic Ig gg 6 B 9g | 8 Om alt SMD em Seta ee eee Il RS SCD SIE opecie Eta ¥g Gg I : 6g | 8 cp | 0 Tae Ra irl oe a oe) Otel elas Guat OO Lg Gg | 0 a. | - | -——-—-- ; ——-f —)— 7 Keay mM $1000 40 qd q0'q 40 “q 83090 10 49 'd “slay af 97000 Dia) spay Omen “Oley §}] 09 sia) a OTe f = OnjuA |Bisouseyy| . omy BOTIIS en[vVA |BIsousuyy| UNIT BOIS OnjVA, |BIseMsey | SULIT] BOLTS on[vA ewly BOIS oOo is \ shes 2h a eek = eah ZF ; HNOLSHNI'] NVISUINOVIV GNOLSANI'T, |) a nn va 374 _ NBW YORK STATE MUSEUM Limestone in excess purifies the iron from sulfur and also pre. vents the reduction of the silica to silicon. Manufacture of basic steel In the basic or Thomas Gilchrist process the furnace or besse- mer converter is lined with some basic material (that is material — containing little or no silica) such a magnesite or dolomite. In this country the latter specially is used. Two things are required of the dolomite, viz, it should contain as high a percentage of magnesia as possible, and it should not have over 14 or 24 of _ total fluxing impurities. It is specially important that the silica percentage should be low, under 4% is possible. At high tem- peratures the lime or magnesia will eagerly unite with any silica present, and as this action is equivalent to corrosion of the lining, any additional percentage of silica will materially affect the life of the lining. Pure dolomites are rare and when found are not always in easily accessible localities, but in this state two different bodies of nearly pure dolomite are known, the. one at Sing Sing and Tuckahoe, Westchester co. the other at - Rochester, Monroe co. For use the dolomite is first burned to the sintering point and then ground and mixed with tar or other material to hold it | together and permit molding. : The lime used in basic bessemer converters likewise has to be of great purity, and the stone must be of such a nature that it will burn to a lumpy and not a powdery lime, for if the lime were added to the converter in the form of powder the strong blast would quickly eject a large portion of it. Sulfite pulp This is a superior grade of wood pulp which is made by the paper manufacturers. In the production of it considerable quan- tities of both dolomite and limestone are used. The following description has been kindly furnished to me by Mr T. A. Howard of the Vermont marble co. The broken stone is thrown into cylinders, eight feet in diame- ter and 20 to 160 feet high. When the tubes are full, fumes of sulfur are led into the bottom and water allowed to trickle LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 30D down from the top. The stone thus becomes slowly dissolved and the liquor is drawn off into storage tanks. This solution is used to “cook” the wood. The latter is cut into chips one to two inches long, and put in a digester holding seven or eight cords of wood. The liquor is also introduced and the mixture heated by steam is under pressure for several hours. The sulfite of lime or magnesia removes all the pitch and everything except the wood fibres, and at the same time removes all discoloration. Some manufacturers claim that the liquor can be made faster and stronger by*the use of dolomite, and in order to get it they sometimes go 10 or 12 miles from a railroad. When limestone is used the cylinders generally seem to be made higher. Inthographing Lithographic limestone is a somewhat impure, very fine and even grained limestone. It is not only rare but valuable. The requirements are sufficient porosity to absorb ink and softness enough to permit working with an engraver’s tool. The chief supply thus far has come from Solenhofen, Bavaria. It has been reported from various localities in this country but never from New York state. Carbonic acid gas Considerable nearly pure dolomite has for some time been shipped from the quarries at Pleasantville, Westchester co. N. Y. for the use of soda water manufacturers. The stone is ground at the mines almost to the fineness of granulated sugar. From the grinder it passes into hoppers whence it is fed automatically through tubes into barrels for shipment. Inme When limestone is burned, that is when it is raised to a red heat, it is dissociated into lime oxid and carbonic acid thus: CaCO, ass CaO + CO, limestone or lime oxid carbonic acid gas lime carbonate quick lime carbon dioxid caustic lime 376 NEW YORK STATE MUSEUM The carbonic acid gas passes off and the oxid of lime remains ae = behind as a white powdery or lumpy substance but may be more or less colored if iron is present. As limestone varies in composition the lime will also-but the Se ; percentage of impurities in the lime will be nearly twice what _ they were in the limestone for the latter has lost 46% of carbonic acid gas. a 3 oe _ Depending on the amount and nature of the impurities present & we may divide natural and artificial limes suitable for mortar into five classes :@ 1 Common or fat limes ja 2 Poor or meager limes | [| ot ae er 8 Hydraulic limes ; ; i ee 4 Hydraulic cements , 5 Natural pozzuolanas The common or fat limes contain less than 10% impurities, and a portion of the latter are insoluble in water, all the rest of the lime being soluble. They do not harden under water but crum-— ble or slake and increase in volume sometimes threefold. They shrink in hardening and to prevent this sand must be added. Poor or meager limes have from 10 to 25¢ of impurities or sometimes even 394. ; | Hydraulic limes are of three kinds: 1 Slightly hydraulic ones with 10 to 20¢ of impurities. 2 Hydraulic limes with 17 to 24% impurities 3 Eminently hydraulic limes with 20 to 35¢ of impurities. All hydraulic limes harden under water. Hydraulic cement is an artificial product. It has less lime than the other classes, but not under 292. Natural puzzuolanas are rocks of igneous origin. They possess - hydraulicity and generally contain less than 10% of lime. It is of course possible to find all intermediate grades between limes and cements. aGilmore, On limes, hydraulic cements and mortars, p. 69. ‘LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUR 377 Slaking. When lime is placed in water the oxid unites with the water and hydroxid of.lime is formed. This is accompanied by the evolution of heat and an increase in volume. Fat limes slake very fast and produce more heat than lean ones. Lime will slake even in the air by the absorption of moisture. If not used immediately it should therefore be protected from the atmosphere as much as possible. Lime may be slaked by putting the lumps in water for a few _ minutes and then withdrawn and packed away to allow the lime - to change to powder. The common method usually employed in building operations is to mix the lime with water in a box. -Too much water makes it thin and injures its cohesive strength. If the water is added in part and the rest later, the lime becomes granular and lumpy. After slaking sand is added to the lime to make mortar. Ac- cording to Gilmore? the lime forms both silicate, carbonate and hydrate, and the crystals of these compounds interlock with the sand grains, thus binding the whole together into a solid mass. In the course of time all the lime changes to carbonate, but this change may take a number of years. Slaked lime is used for a variety of purposes. Its chief use | is for mortar. Quicklime is a very strong base; it displaces car- bonates of the alkalies and serves therefore for the manufacture of caustic of potash and caustic soda. It precipitates magnesia from solutions of salts, and has a use in the manufacture of am- monia from ammonium chlorid. With chlorin it forms chlorid of lime, and with other acids various salts of lime. In the manufacture of illuminating gas it serves to purify the gases from carbonic acid and hydrogen sulfid. It is used in the manufacture of soda and in the extraction of sugar from beet juice. In candle manufacture it is used to saponify the fats, in tanning to remove the hair from the hides, in bleaching, and in dyeing, as a disinfectant; it is also used to treat cryolite in the manufacture of alum and in the production of fertilizers. aOn limes, hydraulic cements and mortars, p. 299, 378 NEW YORK STATE MUSEUM For the manufacture of lime many different types of limerocks— Reet are available, those only being excluded which are contaminated with clay, for this latter substance often affects their most im- portant properties. It is only in later years that the applica- a bility of limestone with a large amount of clay has been recog- — nized. The lime made from pure or nearly pure limestone may be called air-lime in contradistinction to hydraulic lime made from aluminous or clayey limestones. As before stated pure limestone consists of 56% of oxid of lime (CaO) and 44% of carbonic acid. The change from car- bonate of lime to oxid of lime occurs during the burning, the carbonic acid being driven off at a higher temperature. In this process the lime loses about 44% by weight. . As it is generally in a somewhat moist condition when it is put into the kiln, due to water in its pores, the loss in weight may be still greater than mentioned above. The percentage of moisture in limestone is very variable and depends largely on the hardness and density of the rock. The denser a limestone the less porous it will be and the lower will _ be the percentage of quarry moisture in it. | The looser or more spongy it is the more moisture will it ab- sorb. Marl or chalk may be looked on as the loosest form of limestone and in them the moisture may reach 36% or 404, and in — marls and bituminous limestones the loss in burning may be still farther increased by driving off organic matter. A dense limestone is much harder to burn than a loose ee one, and requires more fuel, but this increased consumption is more than made up for by the quality of the lime obtained. In a clean, dense limestone the percentage of quicklime may be 54% while in a bituminous one it may only amount to 30 or 35%. In addition to the decrease in weight in burning the limestone also decreases somewhat in volume as much as 12 to 21% but usually 16 to 184.¢% aC. Schoch. Die Aufbereitung der Mortel-materialien, p. 57. LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 379 In burning it is important to observe that the temperature re- mains as constant as possible and varies only between certain limits. When limestone is overburned, the lime made from it Slakes slowly and incompletely. In the case of limerock with clayey impurities a sintering is very apt to occur and this should in all cases be strictly avoided. : It is true that the higher the temperature is within the per- missible limits the denser will be the lime. On the other hand the temperature must not get too low, as in this case any large pieces of limestone that may be in the kiln will not become thoroughly burned. The unburned core resulting from under- burning makes the lime lean. To avoid such an occurrence as far as possible it is advisable not to put too large pieces into the kiln. The burning should a as rapidly as possible for if the limestone is subjected too long to the highest heat of the kiln the lime will be of inferior quality and will slake more slowly. Limestone begins to lose its carbonic acid gas at about 750° F. but all of it does not pass off probably till the temperature of 1300° to 1400° F. is reached. Limestone should never be burned with a coal running high in sulfur as the latter unites readily with the lime forming cal- cium sulfate. This sulfate of lime reacts subsequently with the aid of moisture on any alkalies that may be present, with the formation of alkaline sulfates, which being soluble are often brought to the surface after the lime is in the wall and cause the oe : white coatings on bricks. | The lime thus’ obtained by the burning of limestone is a white, amorphous, more or less dense mass with a specific gravity of 3.09. It is infusible. Lime weighs from 1400 to 1800 lb. a cubic meter, the variation in weight depending on the density of the original rock and the degree to which it has been ‘burned. Dense stone gives a denser lime. Quicklime is a strong base and absorbs water with the great: est avidity. In water it forms a milky liquid known as milk of lime. 380 “NEW YORK STATE MUSEUM Lime in its normal condition and when dry is totally unaffected te 3 by carbonic acid gas but when heated takes it up rather quickly. — a 3 The addition of water to lime can be done in a variety of ways, ae according to the degree of slaking that is to be brought abouLarrn If a lump of quicklime is immersed in water for. an instant Vg oat saturates itself at once with the former, and this absorption is accompanied by the evolution of heat, a swelling and bursting © of the lime, and the latter finally falls to a fine powder, the hydrate of lime Ca(OH). The chemical action which has taken —_ place is expressed by the following formula. sees Eons CaO + H,O = (Ca(OH), This method of hydration is considered to be better than pou ing the water on the lime. The hydrate of lime thus obtained is a fine white powder of a specific gravity of 2.1. Its water of hydration is pretty firmly combined and is only driven off by reheating to redness. On the other hand quicklime can be made by adding the lumps of lime piece by piece to the water till a strong paste is formed — x . by stirring the mass. The stirring is specially necessary in the © a case of lean limes. | aS In order to assist the slaking of such lean limes it has been found advisable to use only one third the necessary amount of water at first and add the other two thirds later on. Again, as — the lean lime gives out much less heat it is well to keep the mix- ing pan covered in order to prevent its escaping. Lean lime also slakes better if a certain amount of fat lime is worked in with it. The latter has a sort of contact effect on the former, which. is effective and rapid. This method is a good one to follow in using overburned lime. An excess of water in slaking is undesirable, as it only tends to lower the temperature of the mixture. It is sometimes desirable to use hot water. : The hydration of lime powder or slaking to a pasty mass must be carried out very carefully, as otherwise, specially in the case. of overburned lime, some unslaked particles will remain, which may slake later and make themselves unpleasantly prominent. LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 381 ~ During the slaking process the lime absorbs a large quantity of water. It swells up and gradually forms a stiff paste, the - more so, the purer the limestone and the fatter the lime. _ With careful slacking, 1 cubic meter of fat lime gives 2.7 cubic meters and 1 cubic meter of lean lime gives 1.8 cubic meters of paste. and is also drawn off while the slaked, pasty mass is allowed to stand in the pit to insure thorough slaking of every particle. In the pits lime will hold itself for a long time without change provided it is properly protected from the air. ~The damp lime paste absorbs carbonic acid greedily with ie formation of carbonate of lime, which solidifies. The crust of : calcium carbonate which forms is very thin but it prevents the action from continuing farther in the mass. The solidifying action of the lime alone is of little pnoreaec and becomes of value only when sand is added. The use of the sand prevents large masses or lumps of the lime from collecting in any one spot and not becoming thoroughly converted into the carbonate. ; USES OF LIME: Sugar manufacture. Much lime is used in the manufacture of beet sugar and here again the raw material must be of the proper composition. Both clay and sand are injurious impurities as they increase the loss in lime in making the limewater and the clay also introduces alkalies into the sugar juice. The sugar manufacturer considers that every part of insoluble matter means a loss of three to four parts of carbonate of lime. When therefore a limestone containing 95% carbonate of lime is paid The excess of water is gotten rid of in part by evaporation / for as if containing 100%, a stone with 852 should only be paid - for as if containing 60 to 70%. If the lime is to be used for sepa- ration the presence of much magnesia is injurious for the reason that it will not unite with the sugar as the lime does, forming a monosaccharate of lime which is essential before precipitation takes place. Consequently a large amount of magnesia hydrate in the lime necessitates the use of so much more of the latter _and may also cause loss in sugar. 382 . NEW YORK STATE MUSEUM A limestone to be used in sugar manufacture must not haye more than 254% alkalies. | The following are analyses of limes used by German beet sugar manufactures. (Thonindustrie Zeitung, 1897 p. 1165) : Cad re oe MgO Na20 Has SO, Lamhamn, Sweden... 2° -9).°60°" (1762-9: 79 3 | Plymouth, Eng....... 95.22 2.44 : Goon, Ger: (2). 42 -° 89.82 798. 404 ees : Gr. Kunzendorf, Ger.. 96.66 1.10 .86 .05 Ober-Kaufiung, Ger... 97.72 1.20 .70 .06 15 Kosen, Gers. 204i 2. 97.00) 1252) 2. OF Osterwiek .. 2. 0c... 932065 25.8 | pees aiken 22S re 90 127 20 SSO eee PMEZOMUOEL #2) sees 89.04 8.80 1.24 .05 much much Orneres se che 18,94 18200 2.94 ~ 206 Riidersdorf.......... 94516 3° 22008 F74s 2 aS It will be noticed from the above analyses that in most of the samples the percentage of lime is over 90% though in some it is under 80%. Another noticeable feature is the low percentage of both magnesia and alkalies, specially the latter. One shows the presence of much H.S and another of appreciable amounts of SO. “It is the custom for beet sugar manufacturers to burn their own lime for the reason that the carbon dioxid gas is also used in the process. For the production of the best results it is therefore important that the limestone should be of proper quality and the burning conducted in the right manner. Silica is a deleterious impurity as it not only causes the stone to fuse but also lowers the amount of lime and carbon dioxid produced from each ton of stone used. This latter point is of course true with regard to any other impurities which may be present. Too little fuel should also be avoided as it decreases the amount of CO, produced. LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 383 The stone used should be compact and hard. An excess of moisture, as 5% or over, should not be present as it reduces the , _temperature of the kiln when first charged. Stone containing an excess of moisture also tends to split in burning. About 1% of water is the proper amount. - Magnesia is not specially objectionable except when silicates are present in the stone; it causes difficulities however in the purification of the sugar juice, consequently it should be at a mini- mum. Sulfate of lime may act the same as magnesia. If silica is present part of it passes into the juice with the lime and retards the filtration process- by coating the cloths in the ‘filter press. Silica also forms part of the scale on the heating surface. There is less harm from this source in hard than in soft stones. | Silica and alumina also tend to form an insoluble coating on ‘the burned lumps which interferes with the slaking. The following analyses together with most of the above in- formation on the stones used are from the report on the beet _ sugar industry of the United States, dep’t agriculture 1897 p.. 205. 3 1 2 3 4 5 G6 q $ | 9 10 WIOESUUTLE ‘oo seis esis sinja:e, stoic ce occ 4. LO Halon keep 4.15 4.17 6.25 5.16 52 | 1.21 11 MBM ee a lclanislarc.s byes OSes? ais 4.50 5.15 4.90 | 2.15 3.07 Sali 2.25 85 5 27 Organic Matler so: 6.2. feds cee ilerADe | Shea bey 1.37 1.05 97 1.12 .86 .30 41 15 Solmble siliGal. secs nein costs oes 2.10 1.75 3.30 1.05 98 64 -56 .06 20 03 Tron and alumina oxid ....... she 41 20 a7 19 15 .20 Jo2 Done teat Lime carbonate.............2- 85.86 | 85.12 | 81.67 | 90.13 | 88.65 | 87.93 | 90.03 | 93.80 | 96.58 | 99.10 Magnesia carbonate .......... 95 47 .59 05 OD .50 -45 1.81 SS Seon PANE RNICS rersanistas eves s naeleisis eels -05 LOGS aerate .10 AO LEG I ere aielocs, Silheie teas Sherel| er eeereaters OE aa Of the above nos. 1, 2, 3 and 4 are considered bad; 5, 6 and 7 are passable; 8, 9, 10 are excellent. No. 3 was used in a sugar factory and caused trouble, notably “scaffolding ” or difficulty in the mechanical filters. No. 9 was ‘substituted and these difficulties disappeared. In looking over the analyses of limestones given in this report it will be observed that limestones of as great purity as nos. 8, 9 and 10 in the foregoing table are not uncommon in New York state. There are at present two beet sugar factories in New York state, the one at Binghamton and the other at Rome. 384 NEW YORK STATE MUSEUM. The following are some additional analyses of limestones used in beet sugar manufacture. Nos. 1 and 2 of stone used at Los Alamitas, Cal. and no. 3, a French stone. No. 1, the Colton stone, is good No. 2, Oro Grande, is passable lax J - No. 3 is bad. ; : 1 2 : Lime carbonate ............ seeetes+s 98.000 94.306 © Sictue Magnesium carbonate ........:...... 453 1.845 2.50 - = from andsaluming OxId:.) 2. as ee 1.096 -929 WPA RE oS Sooiliea, sand, etc... <7... ss ace ee 281 900. - 82a eMonstures ol ey ee 051.088 — «5.25 Organic matter and magnesium sul- PARE eee Vise eee Oe ot a eee HOM Benge SRE 701 L231 Wandewermined (8. aa 116° 1 et 64 _ ‘Chlorid of lime. Lime which is to. be used for the manufacture of chlorid of lime must be very clean for on this hangs the possi- bility of making a strong and stable chlorid. To satisfy these requirements the limestone must be sufficiently pure and burned ss as well as possible. For this reason many manufacturers pur- chase the limestone and burn it themselves. The burned lime should be free from carbonate of lime, and the limestone should have a minimum amount of sand, clay or similar impurities, which in burning do not of course turn into lime. Aluminous limestone clears with difficulty when dissolved and hence is not 33 liked by bleachers and paper manufacturers. As the consumers require a pure white lime the stone must contain- practically no manganese or iron. These metals are also thought by some to injure jts stability, but this point is not defi- nitely proved. The presence of magnesia is also undesirable as the greater deliquescence of the magnesium chlorid renders the lime chlorid less stable. , | The presence of organic or bituminous substances in the lime- stone is entirely harmless as they do little more than impart a dark color to the stone and pass off in burning.? * aWagner. Chemische technische Untersuchung’s-methoden, 1898, p.430. ae Se SS i LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 385 Fat limes which slake quickly and fall easily to a fine light powder absorb chlorin much quicker than lean limes, which on slaking give a sandy powder even when analysis points out each as almost pure and shows no difference. In addition chlorid of lime made from fat lime keeps much better than when made from lean lime (Wright, Chem. news, 16:426) Glass making According to Mr J. D. Weeks® lime is of considerable impor- tance in glass manufacture. “Glass rich in lime requires a higher temperature to melt and because of this is more destruc- _ tive to the pots, but used in proper proportions it promotes the fusion, aids in the decomposition of the materials, and improves the quality of the glass. Lime glass can not compete with lead glass in brilliancy, but it is harder, not so easily scratched, holds its polish longer, is more elastic and consequently tougher, will stand higher temperature, resists the action of water and chemi- cal agents and is much more cheaply produced. Lime glass also on account of the slight difference in specific gravity of the two substances composing it is less liable to become striated. In the manufacture of plate glass, which is ground and polished, it is found that glass which is rich in lime is harder to polish than that poor in lime, but it holds its polish better and longer.” It may devitrify from the presence of excess of lime, as when an ex- cess of lead or sand is used. The lime should be as free from impurities as possible, specially oxid of iron. Below are given two analyses, no. 1 from Blair co. Pa. and no. 2 — from Sandusky, O. The former is used for window glass, the lat- ter for lime flint glass. 1 2 BRE ARMIN EET in: og os Sto avis Sin v wis a \S eet. 0.8 whe 09 .05 SLND a > ee Mortar The use of lime as a mortar has been known for many years, and the ancients were familiar with the fact that by means of 2 simply burning limestone and soaking the burnt mass in water they could obtain a stiff paste which possessed valuable prop- erties. | | Lime is extensively utilized for mortar making at the present day. : Pure CaO has 71.4% Ca and 28.6% O. It is a porous, earthy, white solid, which when pure resists a high degree of heat. It absorbs both moisture and carbonic — from the air with the greatest avidity. Richardson gives the following requirements for caustic lime ~ used for mortar.” 3 Except when made from coarsely crystalline marble or from marl or shells it should be in hard lumps. It should be white, or nearly so, in color. Lime of a yellow or brownish color with veins of siliceous matter is inferior. It should be free from fused or semi-fused stone which shows | | over burning, and from unburnt ash of fuel or clinker. } It should contain less than 10% of impurities but often has more. It should slake rapidly, showing that it is rich and fresh. Good lime in lumps should weigh, as packed, with about 40% of voids, 60 lb. a cubic foot, 75 lb. a bushel and from 220 to 230 lb. a bbl. of 8 bushels. If ground or in powder it will weigh less when packed loosely, but when well shaken down it will weigh as much as 270 Ib. a bbl. A lump of hard lme 1 foot cube would weigh about 95 lb. having a density of 1.52. Slaking Lime combines with water with evolution of heat and every 100 parts lime take 32 parts of water. aBrickbuilder, 1897, p. 78. “~~ - LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 387 If 33¢ of its weight in water is sprinkled on lime it heats, cracks open and falls to powder. : The increase in volume in slaking is caused by the expansive force of the steam. Lime may be slaked without increasing its volume by passing dry steam over it in a tube. The energy of slaking increases with the decrease of impuri- ties. The same lime may show a varying increase in volume in Slaking due to amount of water added, etc. The slow addition of water raises less heat. Slaking lime in an open box gives less . heat than in a closed one. | With an equal volume of water the increase in size of a rich lime is 2% to 2.44. Richardson illustrates this point as follows: Vol. of H,O | Increase in volume 3 ae: 1.6 | 1 epee a4 | 2.5 With a poor dolomitic lime it was 2 ; gy No set rule can therefore be laid down. For instance 1 peck lump lime with 44% of voids, on slaking with its own volume of water gave 27 pecks of fine powder of slaked lime. From 1 peck of closely packed lime, 2.5 volumes of slaked lime were obtained. | Gilmore found large increases, some running 2.46, 2.83, 3.21, 2.40, but this was caused by his using larger amounts of water than are generally taken in practice. The following table gives the tests made by both Gilmore and Richardson. Rockland Rondout New York penne Richardson Meioire Ghalitreriih Mie oe h 5 oe ake s ie 5 ees 5 GU OMA THEC IME G6 260. 5,9 fo. tie tooo 1557 1806 2350 Vol. of water required to slake......... 2988 3300 2000 Increase of weight in %.............:. 2.24 2.24 1.60 PHCLEASG IH: VOLUME. 3%, os «ok oe oe 2.46 2.14 1.91 Ea ow en hie s teres? 388 NEW YORK STATE MUSEUM The theoretic-increase is 1.53. Lime also slakes simply on ex- Aes posure to the air but it is not good for mortar making as its slaking has been accompanied without any violent disengage- ment of heat to rupture the mass. ee The larger particles also have a hardened rim. Method of slaking. The water may be sprinkled over the lime gradually, or added at once in excess. The former is best because a looser mass is ‘obtames and it - gives better results with poorer limes, slaking them more ~ thoroughly. Too great an excess of water tends to lower the temperature and render the slaking incomplete. This latter causes unslaked particles to get into mortar, and by their subsequent slow hy- dration and expansion they may do much harm. Popping of ~ mortar is due to this cause. . It is also true that if the water is added gradually it may allow the mass to cool down. Enough water should be added to allow for that escaping as steam. With very fat lime 24 volumes of water may be taken. Poor magnesian limes take less. Pure water should be used. That with soluble salts gives rise to efflorescence. Hence sea water can not be used though it has ~ been successfully tried for hydraulic cement. An excess of water gives granular paste and also makes the mortar porous. In making mortar the sand is added to lime for economy and to prevent shrinkage. Sand should be clean and sharp and should be in such quantity that the lime will fill all the interstices. If an excess of sand is used the bond is poor. If too little sand is used the mortar shrinks and cracks. If too little lime is used the paste is made thin. Jn ordinary sands the spaces from 30 to 40¢ of the total volume and in such 1 vol. paste fills voids of 24 vols. sand (Brickbuilder p. 101, 1897). In practice 1.25 to 2 vols. of sand to one of paste is used. This in case of fat lime means 3 to 5 vols. of sand to one measured vol. of lime and this gives a plastic mortar which does not crack. LIMESTONES OF NEW YORK AND THHIR EOONOMIC VALUE 389 Richardson gives following mortar experiments. Composition and physical properties of the lume Mersom-ionition, HO and S........-- Beet ee Sera na aes paren Insol. SiO, and silicates .......... Roe Nas eet ak Sara 1.2 Al,O-; and Fe,O; Fe heme iar eteuldT cube cat apletcae ieve keer a: Tas tre lane er Hel wetiol ae Kee : .8 CaO . e e Sa ete. ef :.€\ (8. @) @ OP Pe OS 8) Va 16) iG)e Oye 8) t SC 8), BQ OS 6) 6 8 ° e es 95 . 6 Weight of cubic feet ineluding voids ................... 60 lb Voids eoreesrke &# @ es eee. se 3 a. 8 "8/0. “e@. .2°@, @ +O. Se ~-8- (8 @ s e eve) 8 eee. 2% 19 eee 44% BOC NMO De oat ek Pe oe Weel oe hot ee le a 1.52 No. of experiment............ deters tee eerie Soin Meee a 2 e 3 4 5. REIN Ol CAOMSCH, CAM TRA eitee ctralolere ealipetesafelslell\iale:s WRIA Ker oNiidic savsicre sieerdinorerae 1891, 6’94 Wiest POrt: CEM. CO... 6.6 osc ees WESEOL MY Se ctcasiae cnretneenle sale WamktoneS2 Dil saisaciticieretioets 1890 Ba CLGETIN 1 SOS oe Caleimia etliate: +.) oriis ors sto. cerase era .18 .16 21 WEA ae oie dialtone ne ashy eacuunes Tah cr rae setere .90 .88 .93 ro (30 C2 eh aD ARUN OCA) Mare ne ta TAM eg ATR ara aie 31 .O9 .46 Water. BOS cr a gs tae cl clan RC NLONREy crac ee) arte ae 1.82 61 .43 aMineral resources of U. S, 20th rep’t U. S. geol. surv. pt 6. LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 409 A clay or Medway mud from Gillingham is as follows: MEMO On aie ory ee cia ese je te 38 13 | Sand Plmimiva and ferric -OXId ow eel 1.856 Ee 5 Suh NRCG Nt ee a ae iage ere 95.249 | SeMnOMEMRU ee Ketch ide CRE TS hes ala Uae Sony 14.244 | PMMA ne Smet TS i ETN os 6.744 | NPS LUN noe eS USN aN os UA a Nik .810 1) DEEL GAA NO IR a a 172 ees PeGiasi wk... 1 cf Tcl ge eas Vaeeaget Ree 20Ooe | RRM e UR io cad ae Re de 773 | merce e hfe et AN RR Pe MOR 3.384 eee THA POS Se a Be Phe eRe 214 | Clay used for the manufacture of portland cement should not contain an excess of sand nor iron. Clays low in iron are usnally of a gray or blue color and light yellow on weathering. The clay should be fairly siliceous, and the more amorphous silica present the better. Michaelis (Hydraulische Mértel u. Portland-Cemente, p. 99) gives the following typical examples: 1 r-4 3 4 5 6 BNA a2 3 o'ee ew 60.06 59.25 60.00 62.48 68.45 64.72. (2) Ue WF G92 23 12 9 OB 2290 OO; I 64 2a Oe Herric :Oxid: ..'. ;.. TOSS 28250378 O00 Coo IE 80n ey Gre 2 ee 0) OD grea Was Tos 6 80") 5/0 a, teen Mesa wer ree. 5 1. SON DB Or LOO A LG) peri BPOuAgES.. Sd. eae 5 2 Oem (es co eA Onc Meg de oe ON) ee eas Bears on ae Y's a Maa LOO 12 coulis toe ROL ae aa Calcium sulfate .. 60 2.73 .89 BOO SSN ye eae 1 Province of Saxony...... Rept SE a eis 4 Mark Brandenburg BEEN OL BORIMACTI 6) ie ecs 6 sas oa Dhara 5 Medway Fs GSE Se SCS sh eal a a 6 Cements high in alumina have a tendency to expand and to blow or to check. Magnesia is also supposed to cause expansion | after a lapse of a considerable interval, while sulfates are looked on as causes of disintegration of portland cement when exposed to sea water. Cements low in lime and without an excess of alumina but high in silica are simply of low strength as under burned cements. If the alumina goes above &@% it is considered 410 NEW YORK STATE MUSEUM high, if below 5¢ it is considered very low. Mr Richardson con- siders that over 3% of magnesia is an excessive and undesirable © quantity,and the proper limit for sulfuric acid is 1$¢. The follow- ing are the percentages of magnesia and sulfuric acid in portland cements which have been placed on American mae during ie past few years. . MgO SO, 86 ) 1.25 | 2.79 vel 1.81 1.24 1.45 1.1 1.68 1.50 2.48 1.36 2.84 1.53 1.16 Mra 2.73 1.51 1.85 1.39 152 132 Specific gravity of portland cement. This is ascertained by deter- mining the volume of an oil which does not act on cement, such © as dry oil of turpentine, displaced by a known weight of cement, For rapid work in the determination of the specific gravity of cement a form of volumenometer has been devised (Min. Ind. 1896, 5 p. 81) which is considered to be free of most of the de- fects found in those generally used. It consists of a small flask with a short slender graduated neck; the lowest graduation. mark on the neck is 14 c. c. and the capacity of the flask is known and equals 64 c. c. The instrument is used by running into it a 50 c. c. oil of turpentine from a pipette which has been accur- . ately calibrated against the flask. As the oil of turpentine is introduced by the pipette the neck of the apparatus is kept dry and the known weight of cement, viz 50 gm can be readily added through a small funnel without blocking the tube. The shortness of the neck conduces to the easy introduction of the cement. The plan of first placing the known weight of cement in the flask and then running in 50 ¢c. ce. of oil appears at first ds pie ea aa aa fe ih Iwi LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 411 sight preferable to the method described above but the complete displacement of the air entangled in the cement is less easily accomplished than when the cement is showered down through the liquid. The temperature of the oil of turpentine must be known but need not be fixed at any standard point, and after the operation the volumenometer, which is stoppered to prevent evaporation, is brought to the same temperature by immersion in the same vessel of water as that used for the stock bottle of | turpentine. All hydraulic cements have specific gravity such that the displacement of 50 gm falls between 14 and 20 cc. c. This renders the graduation of the stem ample, but it is obvious that with any material differing largely from the specific gravity of three, more or less than 50 gm can be taken so as to bring the displacement within its range. Good well burned cement as it comes from the mill has a specific gravity of less than 3.15. It is generally higher than this and may even reach 3.20. The specific euavily falls rapidly when the cement is aerated. 7 Structure and color Even when ground to the finest degree portland cement shows sharp grains. Toa great extent the color of the product is pro- duced by a combination of the shades of the individual grains. Naturally portland cement should be white but this becomes: covered up by the colors of the iron and manganese compounds formed during the burning. Furthermore when fluor spar is used as a flux it develops a dirty grayish brown color in the clinker. Sometimes the color of the cement is changed artificially. Tests In addition to the tensile strength test of portland cement the hammer test is sometimes tried. A machine has been devised known as the Béhme hammer machine, which consists of a hinged hammer operated by means of a spur wheel. This spur wheel is turned by means of a crank, and the wheel acting on IU Ree ee 412 NEW YORK STATE MUSEUM the hammer causes it to be lifted and dropped in rapid succes- sion. The hammer weighs two kilograms. - According to the speed with which the wheel is turned the hammer can be made to deliver a greater or less number of blows within a given period (Schoch p. 241). Setting strength. It has been found that the final strength which different cements attain in the process of hardening COr- responds with the rapidity with which they first set. For in- stance a cement which sets very quickly and which may attain — great strength in a few hours will not as a rule compare favor- ably after a month or two with one which sets slowly, while portland cement hardens much more rapidly than natural cements but sets much slower. Of course there will be a varia- tion in this respect depending on the brand of the cement, and those which are considered the most desirable are those that con- — tinue to harden after a long period. According to Mr Richard- son,” American portland cements seem to gain most of their strength in a few days, while the German brands will be inferior in strength at the end of 28 days but will continue to increase for nearly a year afterward and finally attain an equal strength. Even within the narrow limits of composition allowable for good portland cements there is still a chance for variations which will produce marked differences in character. Some of these varia- tions have been noticed. The set of cement is much influenced by the amount of lime specially when the cement is under burned, or by a large amount of alumina. As a rule the more lime a cement contains the harder it is to bring about the proper com- bination in burning and the higher the temperature and the longer the heat that is required. When properly made cements with a high percentage of lime set more slowly but are stronger and better for ordinary uses. Composition of American portland cement The American portland cements are made from a variety of materials which resemble each other chemically rather than geo- aBrickbuilder, July, 1898, p.147. ~ LIMESTONES OF NEW YORK AND THEIR ECONOMIC VALUE 413 logically. As the cement is made from artificial mixtures it is frequently possible to use all grades of limestone and clay bear- ing rocks. Though portland cement is made at many places and from material of widely different character, portland cement materials are not so very numerous and the raw products have . to be mixed within narrow limits. The following analyses are given by Lewis in volume 7 of the Mineral industry, the European being given for the purposes of comparison. Following them is also given a table showing the composition of both the American and European brands of cements. ‘A “WM “3suy “wy “do1g ‘19UUeIg a [Sue S.J p AVAINS ‘10983 "eq o 86°9» "0D 0 ° ea PS a OBL g [orcccfrrtc epee tre: Jerre ete “**=s+log-y Goer let 4g fitsetereseress Leno segueyay Figg) pied a Nae [ce anes ee orca BET. eee eulinc: ““**"l7e°@ 66's log'eg [ooo vrrseses Kero sesueyry 2 CCDS Rehr aca Ooi PPR ee ar 90°T cores = ss egnng 0ST BG's 60°9 perrst stress: ieyo sesueycy 2 ee ee ee lion ear tee bpp ites “jjeqe sesuesiry P80 GI SOR Sy ap seme ane EQ°T sieeiisiisP vant Cea Shai s asi 1G'°F 96°81 86° LG she ned. 0) eine "++ AeqTo ‘d "Cg “Oy yUe o pes te eo Dr ewemawelia: 5 kes Siete eaecenie cue tecaier |teok “lee ey Soa, 06° Tabect pecs Pe Oe yeyo -q “Gg ‘uoyyue 7 . p aartelRaloll,amatienae sbi (tslastamen oie See NV es ICR CLS CLS Te eye “q “9 “aoqae x 2 WGe) oe Gp bee es 96° ye SE ee) Seon dee O1eco SOS ROE ‘TOUN ‘aosuoig 2 6G ee YO ee ee on a Boeck OS I pe GON Ge iG mae ae GO ee aces * 7B "TOU, ‘uosuoIg Z S P06’ TL bitten stielce’l Wektoise (se lists eee ke aes ee “Se 0686 06° IT OL° #9 ee i ‘¢ ‘kysnpurg : 2 MET L 8ST Ice: Gaus ec: Py ira Fey ee | sees Po ae ent ‘0 ‘Aysnpurg : PNG’ 8 siatie Koisie! | faeret a Brae sa lt uammerieratte ay eon ORD 08° GZ G6’ 0G OF OF EO Sek ENO we ** Avyo rx aN ‘STOUT AA DR OF9'F bees erat re eee gas Ne vations OL’ Oe. ext eat ete * [reUL Oe ‘SIOUIG id Matas de aera A i OU age A are Oa £Q°G Aardiece rege GL QZ VG GG: Vee Avo x N ‘S112 S9L9 5 1e°3 9) 0g" ae neyo eae QG°] see Nea qT og oa ee aveneTis es 0e'e@ ** * 9U0]80ULT] aT NI ‘STRAT sudpy tH p a ugs Saket’ |Leemt ob etet! alec cuers's airs eee ce ea eo Oe: e) $9°9 OL’ FL “*** GXTUT "UHOO “ “NT 00 TOLIR A, 3 280° ess LO ONBY "eta ies 6 ele ligt 6. eee, acln, oe ene 00° T ee eee Lt 06 liphele 1S" VL oe een eral ‘OO OOUDIM'T = 29B8'T CPO Ome ee clCneCn Cait eye ancac ers ie Ea 8 gE OH GG ce Qe°T Yors 16° ST “9X10 “WI90 Bq “ATIC A yoyo] (Does es a ead [Oe al (cca OSS OSI ayereye 6S°T 1Q°G ** QuOysOULI “eT ‘KoTTe A ysiqoT oge°T fcc verse loge egg es 954), ee aoc: 989 T ft lese foc tygre [ees slog- eo ier ge: yor yusued “vg ‘AoqTTB A. yeryeT 89° FL |yoor yuomeo ‘eq ‘Aay[v A ysryary 1d ah Freee . ~ + as a ioe z > ag Ot Tee PN SS et Ce ee T= 3s ; y eS : - ng ey REDE Fy, 2 A494 NEW YORK STATE MUSEUM ~ done. Because of the simplicity of the means employed these : mills have evident advantages. er , A rather singular omission in American grinding plants is the absence of separators. In gradual reduction of materials the use of separators to remove the fine stuff before the material — passes to the mills is advantageous, because it relieves the mills fe of that much material and increases their output. Wind sepa-— rators are very generally used abroad, but are not common here. The fineness of the best American cements is unsurpassed in = any practice and as a general average is superior to foreign-made — cements. The following table gives some comparative figures in this respect: | % passing sieves no. 50 no. 100 no, 200 DAW IONS os. Sarai: aia tee oath ey ei aneeet 100 96.4 GiBtt ea ae Sats Pee een oe a. 5 aoe 94.9 BORLA eo wie ele, ask we eae ee 99.5 92.7 cup iclree ca i ha. adh Srercoay« Stee RO LObD PS te 99.7 94.8 PV GNGeINUO ois. ort i ck ee mee ete 99 6, 95ad RMN UGK