. (4-© SPALL ES’ be Lh D Mees panne” . * * | a . ‘ vs \ i SE CoO SSS DODOS DE SOLOS LO OCIS SECO Sos ott Sai CEOCOCS SOOT OS SOO CGT STNE See SG a ; : WR j > ogee’, + eae NY SY SS \ SS QQ \X KG SS \ SS RQQgg S NS SOY MG QV \\ YS \ SS . \ S \ D’WQK \ << ; ape ee el \ SS GE \\ AY SSS AA ESSE eer mee of Aeon ; ihe UNIVERSITY OF THE STATE OF NEW YORK JOHN M.CLARKE NEW c I RI ee ONTOLOGIST EW YORK STATE MUSHUM ANNUAL REPORT 1901 . », )\\ ZAM Wahisiih } \ LEGEND Beekmantown ress A y ! yi an , Ws ‘ SY BOUNDARY Potsdam 1 bY UY } 4 y ys Ph TINE —— Fault; light line on downthrow side ¥e Strike and dip ® Horizontal — heeneelic’ JAMES 8. LYON PQGRTION OF S.E.CLINTON AND N.E.ESSEX COUNTIES OO" SHOWING EXPOSURES OF POTSDAM AND BE EKMANTOWN STRATA G. VAN INGEN. 1901 2 1 Seale 62500 1 5 0 be Contour Interval 20 feet - : | ; } . Danan ismean Sea level we (ier eer “UOT eUTIOS oBe1i0d ” _aiSuespenb ueel0 jo deur o1ydes3138.13S fi i a i yg | j iA oy i 4 , ? r aN my wy iver! i \ ( : " iN i Gi iy 1: eae wy Mae, : 4 | UNIVERSITY OF THE STATE OF NEW YORK : JOHN M.CLARKE, = STAUE PALEONTOLOGIST ZBISU) 78°10 enne : 77°30 : 77°00" nea : TTY La endouye: ale me - oh ah ae 43°00) 6 sh Nis AER RH a ening seh pane orouG CINK vane CAYUGA ‘ berate fit om nh 1 WAINFLEET ie oI - Pte IsOUTH tas ro) | 1 a rnberstones i] h | 1 an apway___Sherkston Hy CAYUGA! 4 STRATIGRAPHIC MAP } OF THE it f 7. A\ PA) | =| SAG er: ajar a ale ORTLA.GE.~DANVL SALON, fo st i fi Bf { ponpufha IN WESTERN NEW YORKE gens iP es ra HA Saws elon dre [ by AAR --- 4 (as y = , JOHN M.CLARKE AND D.DANA LUTHER , U = ‘os r : R MAN,’ &. at 90: ine Ty = 1903. Gas i ed . - W---+t— \ Ne 2 es — Sle im 2) eal é N Cas Fs Hi Grimes W Till Dunkirk Portage Wiscoy Laon. y 2 - black shales gray shales shales &flags sandstone ance blackshales sandstone Shales} (-LongHeardSRiffs(?)) r \ ae i) sandstone wi it j Zl == 42°00 73°30' Pan ase a Pe poet ON ON ys a si en eee TH700" 78°30" 78° 10' A = ; : = a -- = THE ARGUS COMPANY, STATE PRINTERS. ? 2 e en, : Published monthly by the University of the State of New York BULLETIN 303 NOVEMBER 1903 New York State Museum FREDERICK J..H. MERRILL Director JoHN M. CLARKE State Paleontologist Bulletin 69 (ee PALEONTOLOGY 9 ar af Gl REPORT OF THE STATE PALEONTOLOGIST 1902 £1992 PAGE PAGE Operations in the field 1901-2................ 851 | Explanation of pretee WORE Loi icy aeledioe's 1239 PORICe WOPK once eee ee ee eee eee ee es 865 \ TEC ee Re eh ale lh Aiea ae sete 2 SE A 1295 Personnel OMATEDOIS UAL Mc © oreeie silsiscle eta asiel -« 8v1 Plates and maps FACE OMOUUNYRAN ES Umereys ers efercae hce.cieg oe's.s 04,00 encle ob eae 12 SenecCaemMastod Oni ook cece. eee 921 Appendix 1: Accessions.......... Cees gees 874 | Mastodon americanus.............0.. 922 PUMEMM RETIN tet ever erences oisss olsen ne ds leiy.e tee aise «oe 8i4 Map of New York showing distr ibution of Purchases............0.s0-e0e eee cee eee ee tees 875 Mastodon remains... ......cccccccccccedecee 030 (UL BGLLCH Choa til ae ere eee ee ieee 875 Lower falls of Hoosick river at Schaghti- Appendix 2: New entries of localities COCR IE SS eetsh Tk nice ee edhe sate vale Cele 934 Alphabetic list of localities. ............... 77 | Dictyonemaslates at Sennen icone ..-- -936, 938, 940 New York localities by counties...... ....- Si}. lIMBctichmites pet AY ~ ck cept eses coe et «4. 960, 962 PRGGX LO GOMMAUIONS. .-.-. 2500.6. «ween wens 880 | Stratigraphic map of Olean quadrangle Appendix 3 - (Pocket in front cover) Dwarf Fauna of the Pyrite Layer at the Sketch map of part of southwestern New Horizon of the Tully Limestone in West- York and adjacent parts of Pennsylvania 967 ern New York. F.B, Loomis............- 892 Columnar sections of Upper Deyonic...... 989 Mastodonsot New York. Joun M. CLARKE y21 | Stratigraphic map of Portage formation -Cambrie Dictyonema Fauna in the Slate (Pocket in front cover) Belt of Eastern New York. RUDOLPH Stratigraphic and paleontologic map of Be- eT DRUIMEUNICANIN Sache psis(aieie.clors crom cp laye ns aeiep, ae cds 934 craft mountain........ ,. (Pocket in back cover) Sedentary Impression of the Animal whose Sections of Becraft mountain Trail is known as Climactichnites. Jay (Pocket in back cover) eR OOD IMO ILE 6 bic os, alais oleic ache le/esn'e wielalelw a.> 959 Ledge of Cobleskill limestone at Schoharie. 1109 Deyonic and Carbonic Formations of Cobleskill limestone at Howes Cave..... .. 1114 Southwestern New York. L.C. GLENN 967 Stratigraphic map of region about Union Fossil Faunas of the Olean Quadrangle. STAIN O Seasis ctesieurelie is, tattle cinerea divs Gieve er steiner ale 1130 OSUNTEIO NS 85 0001 Sy Sane tea 990 Location map of Kingston... .............. 1176 Construction of the Olean Rock Section. - Stratigraphic map of Kingston........ .... 1178 OTUN) MEO ARK Bs ste faces oclc) oes cece sees 996 Structure sections through Vlightberg..... 1180 Stratigraphy of Portage Formation be- Cross section through North hill............ 1182 tween the Genesee Valley and Lake Erie. Section through North hill at White lime PEVACNVAU TTY TEER < <5 ' ieisecteec.cc gece. aes 1000 GUIBAT EN ee ur seis Sag Milani wasn aoe eee 1184 Stratigraphy of Becraft Mountain, Colum- Leperditia bed and “ee prismatic’? cement bia County, N. Y. AMADEUS W. GRABAU. 1030 DEGGS. a sas wee Saoec ewan mee rea ae acme ermcrete nee 1186 A New Eurypterid Fauna from the Base of Unconformity of the Wilbur limestone.... 1210 the Salina of Western New York. CLIF- hesGloty ole cults .eemersaceae cei terse 1212 TREY d]e SVU: Ap ee Re aPC On Ser ne eee 1080 | North end of Glory Hole cut................ 1214 Preliminary Observations on the Coble- Contorted beds over entrance to Glory skill (‘*Coralline’’) Limestone of New EVOLVE MNCs.) .ececs as reels Soa: 1216 MO. (Cl A EPARTNAGEL. .cos.5 sees cee 1109 Faulted and folded beds in face of cliff Disturbed Fossilifcrous Rocks in the Vicin OVeNGIOPY FLOLG INCIIME . wrecciant 5. sete 1218 ity of Rondout N. Y. GILBERT VAN Sections and sketch plan of the Vlightberg. 1220 INGEN & P. EDWIN CLARE ..............5:. » 1176"). Miew of the White lime quarry............. 1222 Torsion of the Lamellibranch Shell. JOHN PAyite Ute SLU UDIN ee ac celetareie cieictcia io) aiaceteimeettaiaiaioretat= oie ever sO Dis CIWS soa cosoah os iso meseibonnd > 2asBeor 1228 | Crustacea....... ... . Some Deyonic Worms. JOHN M. CLARKE 1231 | Devonic worms.. Pe anenls: teeth a ,~ ne ALBANY UNIVERSITY OF THE STATE OF NEV 1903 Mp106m-Mr3-150 | Price $1 University of the State of New York REGENTS | With years of election 1892 ae CROSWELL DOANE D.D. LL. D. Chancellor, Albany 1878 WuireL.aAw Rew M.A. LL.D. Vice Chancellor, New York 1877 CHauncEy M. DeEPEW LL.D. - - - - New York 1877 CHARLES E. Firco LL.B. M.A. L.H.D.. - Rochester 1881. WitLiAM H, Watson M. ASM Dy 2: ~ Utica 1881 HENRY E. TuRNER LL.D. - - - : Lowville- 1883 St Crarr M¢Kunway M.A. L.H.D. LL.D. | D.C.L. Brooklyn 1885 Danie, BEACH Ph.D. LL.D. - - = Watkins 1890 Pruiny T. Sexton LL.D. ~~ - - - - Palmyra 1890 T. Guinrorp SmirH M.A.C.E. LL.D. - Buffalo 1893 Lewis A. Stimson B.A. LL.D.M.D. - - New York 1895 ALBERT VANDER VEER M.A. Ph.D. M.D. - Albany 1895 CHARLES R. SKINNER M.A. LL.D. : Superintendent of Public Instruction, ex officio 1897 CHESTER S. Lorp M.A. LL.D. - - - Brooklyn 1900 THomAs A. HenpRicK M.A. LL.D. - - Rochester 1901 Benjamin B. ODELL jr LL.D. Governor, ex officio 1901 RoBERT C. PRUYN M.A. Side ae teeter - Albany 1902 Wi1i1AmM NorrrncHAM M.A. Ph.D. LL.D. - Syracuse 1903 FRANK W. Hiccrns Lieutenant Governor, ex officio 1903 JoHN F. O’BRIEN Secretary of State, ex officio 1903 CHar Es A. GARDINER LL.B. M.A. Ph.D. LL.D. New York 1903 CHarLEs S. FRANCIS B.S. - - - : Troy One vacancy. SECRETARY Elected by Regents 1900 JAMES RUSSELL PARSONS jR M.A. LL.D. DIRECTORS OF DEPARTMENTS 1888 MeLviIL Dewey M.A. LL.D. State Library and Home Education 1890 JAMES RUSSELL PARSONS JR M.A. LL.D. _ Administrative, College and Fligh School Dep’ ts 1890 FREDERICK J. H. MERRILL Ph.D. State Museum University of the State of New York New York State Museum FREDERICK J. H. Merritu Director JoHN M. CiarKeE State Paleontologist Bulletin 69 PALEONTOLOGY 9 REPORT OF THE STATE PALEONTOLOGIST 1902 To the Regents of the University of the State of New York ~ | have the honor to report herewith on the work of this depart- ment during the year commencing Oct. 1, 1901. Operations in the field 1901-2 Guelph horizon and fauna. In my report of last year I had occasion to make reference to investigations relating to the distribution of the Guelph horizon and its fauna throughout western New York. This interesting congeries of fossils, con- stituting essentially a new element in the Paleozoic faunas of the New York series of geologic formations, had at that time been found only in the vicinity of Rochester, with the exception of an early locality in Wayne county mentioned by Professor Hall in 1848, but subsequently lost. As noted in the report referred to, our effort of that year to locate other manifesta- tions of this horizon between Rochester and Niagara Falls along the summit of the Niagara escarpment was not successful in its main object, though contributing interesting data bearing on the contact outcrops of various formations immediately involved. The horizon of the Guelph lies so involved with the upper beds of the dolomite series which constituted the closing episode of the Niagaran stage in New York, and these dolomites are, notwithstanding their massive and resistant character, so seldom exposed in continuous section, that the few natural cliff exposures through this region are very unsatisfactory for the determination of the contents of the strata. 852 NEW YORK STATE MUSEUM Early in the present season, however, an artificial exposure along the banks of Oak Orchard creek directly south of Shelby, Orleans co., was reexamined and found to contain evidence of the Guelph fauna for which we had been diligently searching. Here a channel has been cut through the natural rock bed of the creek in the construction of a feeder for the Erie canal and drainage way from the Oak Orchard swamp lying to the south, and, taking the exposure at low water and before the vegeta- tion had become profuse, it was practicable to make out the succession of the dolomite series with clearness and also to locate therein two horizons of the Guelph fauna, the lower of which has proved remarkably prolific in organic remains and these of extraordinarily interesting character, supplementing very materially the knowledge we had already derived of this fauna from its development in and about the city of Rochester. It would appear from a closer analysis of these aggregations that the upper Guelph horizon, which lies 30 feet above the lower, is to be correlated with and doubtless is coextensive with that at Rochester. Following this discovery, the attempt was renewed to locate the horizon at other localities, specially in the continuous section at Niagara Falls, and, though here the section is essentially a vertical one and the rocks difficult of access, the effort to locate these horizons in that section proved successful. Similarly, at various localities from Niagara Falls to Shelby near and south of Lockport, Gasport and Middleport, the horizons were followed, and also west of Shelby in the towns of Barre, Clarendon and Byron, at Claren- don there being an exposure of considerable continuity. At none of the localities, however, except at Shelby were the horizons found to be fossiliferous except in the presence of an occasional species of this characteristic fauna. The problems presented by this fauna, both biologic and stratigraphic, have been carefully studied and are embodied in Memoir 5 of the State Museum, which is now essentially printed, and to which > reference is made under another head. The fauna of the Naples beds. In order to help to a conclusion a monograph now long standing, on the Naples fauna of the - Portage stage in western New York, one part of which has already been published, Mr D. D. Luther carried on investiga- REPORT OF THE STATE PALEONTOLOGIST 1902 853 tions in Erie and Chautauqua counties. This study has in- volved some questions in regard to the determination of the upper boundary of the Portage formation which can be fixed only on the basis of the evidence to be derived from the fossils. The organisms themselves are also for the most part undescribed and constitute one of the remarkable associations of fossils in our older rocks. The fauna of the western New York Portage or the Naples fauna has been shown to have entered the State from the west and not to have penetrated far beyond the meridian of Cayuga lake. Its path of migration into the western boundaries of the State is evidently buried at the bottom of Lake Erie; but, to determine whether any trace of the fauna is to be found to the south or north of the lake, some investigations were carried on in Erie county, Pa. to ascertain the significance of the formations termed by the Pennsylvania geologists “ Portage” and “ Girard shales.” The Portage, it has now been made evident, does not there exist, and the faunistic value of the Girard shales is a matter for further study. In Ontario the black shale beds at Kettle Point, Lake Huron and about Sarnia, Forest and Alvinston, which have been recorded as of Portage age, show no definite relations to the true Naples fauna, but rather represent only the con- dition which prevailed during the deposition of all the black muds of the Genesee and lower Portage stages. All these field operations undertaken during the early part of the season were greatly embarrassed by: the tremendous and protracted rainfall, which flooded the watercourses of the country to such a degree that they became virtually inaccessible, and for some weeks it was necessary to discontinue field work altogether. The study of the Naples fauna is now brought to virtual con- clusion, and the manuscript for some portion of it is in the printer’s hands for a memoir of the State Museum. Brief refer- ence will be made to this also under the caption of office work. The “ Hudson river ” formation and faunas of eastern New York. In continuance of his previous investigations of the “ Hudson River ” formation, accounts of which have appeared in various museum bulletins and reports of the paleontologist, Dr R. Ruede- mann was engaged in Rensselaer and Washington counties. he construction of a tunnel for the extension of the water 854 NEW YORK STATE MUSEUM supply of the city of Troy is affording a section rather more than 1 mile in length through the shale region north of the Tom- hannock river and, by the courtesy of Prof. W. G. Raymond, engineer in charge of these operations, we have been permitted to examine the section in all its parts in great detail as the rock is taken out. This section has already furnished some fossils which indicate the geologic age of the shales through which it runs; but, for the most part, the rock section has proved there, as usual in most exposures of the eastern Hudson river shales, comparatively devoid of these conclusive evidences as to its geologic age. The discovery of a profuse graptolite fauna at the Deep kill, Rensselaer co. as noted in my last report, wherein are repre- sented the three zones of the Phyllograptus shales of Europe or the lowest part of the Lower Siluric, has suggested the pos- sibility of producing a map of that region on which may be distinguished all the graptolite bands of the Lower Siluric shale facies. During the present season investigation toward this end has covered the southeastern part of the Cohoes topographic sheet, with the Hudson and Hoosic rivers as western and north- ern boundaries respectively. A discovery of considerable importance for the correlation of the shales throughout this region was made incidentally in the finding, in the vicinity of Schaghticoke, of the horizon of the fossil Dictyonema flabelliforme _ with associated species, all of which are regarded as indicating throughout northern Europe, and wherever found, the top of the Cambric series. This horizon has not before been found within the United States. This is a distinct contribution to the faunas heretofore represented in the New York series. The areal map of the Tully quadrangle. The work on this quad- rangle was virtually done during the previous season; but it seemed, on careful revision of the map prepared, that the strati- _ graphic divisions were insufficiently detailed, and, to carry out a more minute subdivision of the strata based more specially on paleontologic evidence, the work has been reviewed and is now brought to a satisfactory completion. Work on the Elmira quadrangle; cooperation with the United States Geological Survey. Under the same conditions as have REPORT OF THE STATE PALEONTOLOGIST 1902 855 heretofore prevailed in developing the stratigraphic and paleontologic relations on the Olean and Salamanca quad- rangles, we have this year carried forward to completion, in cooperation with the United States Geological Survey, similar work on the Elmira quadrangle. On this work Messrs Myron L. Fuller and F. G. Clapp were detailed by the director of the United States Geological Survey, and this department was represented by C. A. Hartnagel and H. S. Mattimore in the necessary collection of fossils. The area covered by the Elmira quadrangle being in some degree lower down in the rock series than the areas of the Olean and Salamanca quadrangles, the questions which there arose in regard to the classification of the culminating geologic horizons have not been revived in this case. Most of the territory about Elmira is underlain by rocks of the Chemung stage, though at the north, in the low lands and valleys, are small, restricted areas of the Portage formation directly underlying. Sections however do not rise to any considerable hight, so that the hill summits do not enter on the horizons of the Wolf creek, Salamanca or Panama con- glomerates. On account of the simplicity of the stratigraphic problem here involved, the time required for the field work was not long. The area between the Elmira and the Olean quad- rangles is as yet but partially surveyed, and no maps have been made available for stratigraphic work, but it is on these inter- vening quadrangles that we may expect to find additional and important light on the problems which have arisen in the detailed study of the geologic succession in Cattaraugus and western Allegany counties. The fauna and stratigraphic relations of the Coralline or Cobleskill limestone. ‘“ Coralline limestone” is a term applied by Prof. James Hall to a fossiliferous formation in eastern New York which he believed to be the eastern extension of the Niagara or Lockport dolomites of the Upper Siluric. The name was not one of the original elements in the nomenclature of the forma- tions as proposed by the four geologists, though the term was originated by and had been in local use by John Gebhard, the pioneer of geology in the region about Schoharie county where this formation is best developed, and was also employed by 856 NEW YORK STATE MUSEUM Mather in describing the rock series exposed at Rondout, Ulster co. This formation, which is in typical section in Schoharie county, as at Howes Cave and along the Cobleskill, is a dark limestone abounding in corals and carrying a considerable fauna besides, which has been described by Hall in volume 2 of the Paleontology of New York. It is underlain in this section by a mass of 30 to 50 feet of soft gray shales and, further east along the Schoharie creek, this mass is lessened and the shale is of greenish color. Professor Hall regarded this underlying shale as pertaining to the Clinton formation, and, on account of the stratigraphic position of the Coralline limestone and because of the nature of its fossils, many of which he found to be identical with or similar to known Niagara species, he con- cluded, as above stated, that it was an eastern representative of the Niagaran formation not otherwise known in this part of New York State. The value of this determination has been brought into question by several writers, specially as a more careful study of the fauna of these beds indicates, notwithstand- ing its affiliations to the Niagara fauna, specific identities of notable importance with species which occur in higher horizons in the State of New York. Thus we have observed that, above the waterlime formations at the top of the Salina stage in western New York, probably 1000 feet higher than the last appearance of the Niagaran fauna, species occur which are identical with the Coralline limestone species of eastern New York, and these points of similarity have been quite clearly pointed out in a recent publication by Prof. A. W. Grabau. We have had previous occasion also to direct attention briefly to the occurrence of a profuse development of a fauna similar — in many particulars, in a quite pure limestone interbedded be- tween the upper and lower waterlimes of the Salina formation at Frontenac island, Cayuga lake. Now, though the Coralline limestone with its characteristic fossils appears in Schoharie and Otsego county sections to lie below the waterlime forma- — tion as a whole, in the sections exposed at Kingston and tondout and early described by Lieutenant Mather in his report on the geology of the first district, the formation and its fauna apparently make a double appearance, lying at first below the REPORT OF THE STATE PALEONTOLOGIST 1902 857 cement rock, as at Rondout, and then reappearing after the deposition of a considerable thickness of waterlimes, and the second appearance followed again by more of the cement rock. The lowermost of these beds is not the equivalent of the typical or Schoharie county Cobleskill but its fauna carries a much stronger impress of Niagaran age. We are compelled, for purposes of correlation east and west, to designate this bed by a distinctive term and shall call it the Wilbur limestone. The Cobleskill beds on Cayuga lake at Frontenac island are involved in somewhat similar stratigraphic condition to the upper bed or true “ Coralline” at Rondout. We had undertaken a few years ago to work out the various bearings of the data set forth by this interesting fauna and formation, specially its manifestations in central and western New York. During the past season field studies have been carried forward in the eastern part of the State. It is too soon to state definitely the outcome of these investigations; but this much is clear at the present time, that the fauna of the Coralline limestone, in its first appearance in the Rondout section, contains an important percentage of species which have very close relations even to identity with species of the Niagara dolomite. This resemblance is essentially lost in the higher horizon at Rondout which is equivalent to and probably continuous with the typical Coralline outcrops in Schoharie county. Several of these very character- istic forms occur in the Guelph fauna, which we have elsewhere described, and others, as just noted, reappear in a still later manifestation, in fact the final stage of the Siluric faunas in western New York. In the proper interpretation of the strati- graphic relations of these faunas much will depend on the valua- tion of the beds which underlie the limestone in the Schoharie county sections, and which were called and have heretofore been commonly granted to be of Clinton age. Messrs Ulrich and Schuchert put forward, in the last annual report of the paleontologist, in an important paper entitled Paleozoic Seas and Barriers in Eastern North America, the hypothesis that, during this late Siluric period, a land barrier crossed New York State from northeast to southwest, and that the Coralline fauna was a provincial development pertaining to the region outside or eastward of the barrier, while other phases 858 NEW YORK STATE MUSEUM -of late Siluric faunas were holding the ground on the inner or mediterranean side. The arguments in support of such a barrier in eastern New York during various epochs of Paleozoic time are strong and have been well constructed by the authors referred to. Their hypothesis proves of great service in properly construing the long known and palpable difference in the development of the Paleozoic rocks in eastern New York and in the central and western parts of the State. We are disposed to believe that the complete analyses of the proposition now before us concern- ing the value of the Coralline limestone and fauna will throw important light on the existence and influence of such possible land barrier during late Siluric time. We have above and previously used the expression, ‘“‘ Cobleskill limestone,” as an alternative name for this formation, in view of the fact that stratigraphic names seem to meet modern require- ments only if designated by geographic terms. The term “ Coral- line” is unfortunate in many respects; it originally had reference to the abundance of corals in the rock, but the word is now used with a different signification, and, while it has no geographic value, it has neither the biologic importance which such term should carry. The Cobleskill presents the best sections of the formation to be found in the region of its typical exposures. Mr C. A. Hartnagel, who has been specially concerned with the study of this problem, communicates the following account of his field operations: Work on the Cobleskill formation. This report is a_ brief account of the field work during the greater parts of the months of August and September, on the Cobleskill forma- tion. For convenience the region studied is here considered in three sections. First, that extending from Gallupville, Schoharie co., west and northwest through Shutter’s Corners, Schoharie, Howes Cave, Central Bridge, Grovenor’s Corners, Car- lisle, Sharon Springs and the section to the north and northwest | of Cherry Valley in Otsego and Herkimer counties. Second, that — section in Albany county, along the northern and eastern ends of the Helderberg plateau, extending from Altamont, and including the Indian Ladder and New Salem sections, to South Bethlehem. Third, the section extending from Catskill in Greene county, south REPORT OF THE STATE PALEONTOLOGIST 1902 859 through West Camp, Saugerties, Glasco, Lake Katrine, East Kingston and Kingston (Rondout). From Kingston this section extends southwest through Wilbur, Eddyville, Whiteport, Binne- water, Rosendale to High Falls, all in Ulster county. 1 Gallupville. On the left of the road leading north past the cemetery, from Gallupville, at a distance of 42 mile from the village, there is exposed, though somewhat obscurely, the Cobles- kill formation together with the underlying Salina shales. The Lorraine shales are well shown here, as is the Rondout series above the Cobleskill. This is the only section where the Cobles- kill has been observed north of the Fox kill. Professor Prosser, at a point farther west, near Shutter’s Corners, has observed the Rondout, but a careful study of the vicinity did not reveal any outcrop of the Cobleskill. Shutter’s Corners. One half mile south of Shutter’s Corners on the farm of Seth Stevens, occurs an outcrop of the Cobleskill. The weathered condition of the rock at this station has made it favorable for collecting, though here and continuing for more than a mile westward the vicinity of the outcrop is of a swampy nature, owing to the low dip and the wearing away of the softer rock above. Between this station and Schoharie the formation is exposed at several points, and, where not exposed, its position is marked by a small ridge rising above the general level of the land. Schoharie; east side. To the east and northeast of Schoharie, running obliquely up the hill from the African church, is an almost continued exposure of this formation. This outcrop has been noted by Mr Darton, and it is said that most of the Coralline fossils of the William Gebhard collection were obtained from it. One fourth mile east of the postoffice at Schoharie, the shales underlying the Cobleskill are exposed by the roadside, and a few rods farther brings one to the old Brown quarry, at the base of which is exposed the Cobleskill, followed by what is evidently a cement rock nearly 5 feet thick. Above is a limestone in two layers of nearly equal thickness, their total thickness being 50 inches. They here form the roadbed and can be traced a hundred yards farther south to where Mr E. Vroman has recently opened Yroman’s quarry a quarry in them. These layers are worked as “ Coralline.” In- 860 NEW YORK STATE MUSEUM tercalated between them is a somewhat shaly layer with abundant corals. | Schoharie creek sections. On the west side of Schoharie creek, besides the well known exposure south of the creek bridge, the Cobleskill is exposed at Clark’s cave, 14 mile north of the bridge. At this point the Lorraine shales are well shown, and the contact with the Salina shales can be seen. There is another exposure of — the Cobleskill on the east side of West mountain, at the stronti- anite mine 1 mile north of Clark’s cave. Farther along on the northeast point of the mountain the rock is shaly, and collecting is good. Still farther along, nearly opposite Central Bridge, there is a Similar exposure with fossils. From this point to Howes Cave there are no good exposures on the mountain side, and the dip soon brings it below the surface when a lower level is reached. Howes Oave. The Howes Cave section is well known, and from this point the formation is somewhat obscured for some distance to the north, but, at a point 1 mile below and 14 mile from the highway leading to Central Bridge, there is exposed in the creek bed the Cobleskill together with the Salina shales and the Lorraine beneath. This section is one of the best at which to observe the contact between the different formations. Beyond this station and nearly west of Central Bridge, on the farm of Mr Tarr, there occur very large boulders of Cobleskill arranged in nearly a straight line, from which corals may be had in large numbers. A mile and a half farther north from this point the limestone outcrops by the roadside at the house of Eugene Maxwell. The overlying rock has been removed by erosion, and considerable of the upper surface of the Cobleskill is exposed at this point, and on the road to Grovenor’s Corners, where frequent exposures are seen, specially near the house on the Judson Grovenor farm and at several points on the farm of Sol Dewey. Grovenor’s Corners. At Grovenor’s Corners there is a fine ex- posure, and this outcrop continues at intervals for nearly a mile on the road to Carlisle. Carlisle. One mile northwest of Carlisle is the last good exposure of the Cobleskill on the way to Sharon Springs, but there are several points where its presence can be detected and REPORT OF THE STATE PALEONTOLOGIST 1902 861 fossils obtained. But within 3 miles of Sharon Springs no ex- posures have been noted. Sharon Springs and Cherry Valley. At Sharon Springs and the section north of Cherry Valley it is clearly evident that there is no limestone between the Lorraine shales and the so called Salina shales above. Westward from Cherry Valley and extend- ing into Herkimer county the Salina shales rest directly on the Clinton formation showing that there can be no Niagara present in this section. 2 Altamont. In the Helderberg at Altamont, there is a space occupied by an impure limestone which may be referred to the Rondout. ‘This limestone rests on the Lorraine shales. The same condition exists at the Indian Ladder. At South Bethlehem the Rondout is somewhat thicker and it is said would make cement. The contact with the Lorraine shales was seen at this point. A short distance south of New Salem there is a thin layer of sandstone lying on the Lorraine shales and below the Rondout. The sandstone contains iron pyrites, and Professor Prosser has provisionally referred it to the Clinton. It may now properly be included in the Rondout. Catskill. In the region southwest from Catskill are found the remains of corals and some brachiopods below the Rondout beds, and often the corals are directly on the Lorraine shales, which at this point appear to be conformable with the overlying rocks. South, near West Camp, at the end of a syncline extend- ing from the Catskill region, there is exposed in both limbs of the syncline, about 3 feet of the Wilbur limestone. At this station a number of Leptaena rhomboidalis were found. From West Camp south through Saugerties one can only hope to find the Cobleskill in the limbs of the anticline, which passes from some distance west of West Camp through Saugerties and finally into the Kingston region. The western limb of this syncline was not examined, but the eastern limb in the section about Saugerties is eroded, and only the higher formations can be seen. At Glasco there is a somewhat ob- Sscure outcrop, but farther south, beyond Lake Katrine and near East Kingston, there is a fine exposure. About 2 feet from the bottom there is a thin layer crowded with Atrypa reticularis. From this point the limb of the anticline is either obscured by the Champlain clays of the Hudson valley or eroded. At the Newark Lime and Cement Works the Wilbur is shown at several points. Several less important outcrops occur at Wilbur and Eddyville. Outcrops are also found across the Rondout creek opposite Wilbur. These relations hold good 862 NEW YORK STATE MUSEUM almost to Rosendale from Rondout along Rondout creek, but from Kingston through the Whiteport-Binnewater stations the cement lies on a floor of sandstone (Clinton). The cement at Rosendale is also on a base of sandstone, but at this point I have found small Leperditias in large numbers. They seem however to belong to the cement above. At High Falls there is a thin shaly layer above the eaindaee and distinct from the cement beds above. This shaly layer con- tains an interesting fauna and seems to be SEU oe to the Wilbur. It is to be noted that, throughout the cement region in Greene and Ulster counties, the cement beds above the Wilbur occur in two layers, between which is found the Cobleskill containing an abundance of corals, mostly Halysites. This limestone in . the Whiteport-Rosendale region is about 12 feet thick as a rule. However, in the Newark works at Rondout this layer is only 7 inches thick. The faunal contents of this limestone in Ulster county have not been examined in detail but suggest some very interesting studies. ; The stratigraphy of Becraft mountain. Just east of the city of Hudson in Columbia county, is Becraft mountain, which has long been known as one of the interesting features in the Paleozoic geology of this State. The mountain is the only out- lier east of the Hudson river of the Helderberg series of for- mations, on which lie in proper succession other members of the Devonic series to and into the Onondaga limestone. It has been the subject of much study. Accounts and sections were given of it by Lieutenant Mather in his report on the first dis- trict of New York, and he then indicated the essential tectonic structure, which is that of a low syncline of the higher deposits resting unconformably on the upturned edges of the Hudson river slates. At a later date the structure of the mountain was more fully elaborated by Prof. W. M. Davis; and subsequently the writer specially studied an outcrop of the Oriskany sand- stone thereon of new interest in the composition of its fauna, and published a somewhat extended account of this element in — the make-up of the hill [Museum memoir 3]. In all these various studies, however, it has been clear to the observers that we had not yet reached a true solution of the structure of the mountain as a whole. Evidence of faulting and displacement — at the southeast end was recorded by Mather and reiterated by Davis, but it has not been clear how profound were these REPORT OF THE STATE PALEONTOLOGIST 1902 863 disturbances or how deeply they may have effected the rest of the mountain mass. For the most part, the mountain stands with abrupt sides in all directions except toward the southeast, being a wall of Manlius limestone underlain by the Hudson river shales. Such disturbances as it has undergone would be determinable with difficulty except by the aid of paleontologic facts. The interest pertaining to this area, the extensive series of exposures running through a number of highly fossiliferous deposits, the instructive illustrations which it affords of denuda- tion, folding, overthrust and displacements of various kinds and the easy accessibility of the locality have justified a more care- ful study of the area than has heretofore been made. This work has been specially facilitated by the fact that we have been able to plot the results on a topographic map of the area, prepared at the expense and under the personal direction of Dr John C. Smock, formerly assistant in charge of the State Museum, later, state geologist of New Jersey and now a resi- dent at Hudson. The areal work on this problem has been assigned to Prof. A. W. Grabau of Columbia University, who has this season spent some weeks on the ground and has arrived at a satisfactory analysis of the structure involved. According to his determinations, this proves to be much more complicated than had been supposed, and the succession of rocks and faunas there exhibited will, when properly displayed on the map, throw new light on the forces which were efficient in upturning the fossiliferous sediments of eastern New York. Dr Grabau’s work is essentially finished, and his results thereon will be found in another part of this report. | The Westfield mastodon. In the month of June I was informed of the discovery of mastodon remains in the village of West- field, Chautauqua co. Such discoveries, though of frequent occurrence, are worthy in every case of investigation and record, and in this instance the situation was as follows. The bones were accidentally discovered while an excavation was being made on the property of Mrs Alice Peacock. The lot in which they were found to occur lies along the Nickel Plate Railroad, and is bounded on one side by the barn pertaining to the prop- erty and on the other by the highway. Across the highway is a low swampy area which extends for some distance to and 864 ‘NEW YORK STATE MUSEUM beyond the railroad right of way. In digging over Mrs Pea- cock’s lot for the purpose of constructing a fish pond, bones were found lying on a pavement of heavy stones and just below a thin layer of muck. At the time of my visit on July 4 there had been taken from this excavation, one tusk, a number of ribs and vertebrae, part of the scapula, pelvis and sacrum. The ground had then been well dug over, and the prospect of finding other bones did not seem altogether favorable, nor had enough been secured to make the acquisition of them particularly de- sirable. It is quite probable however that more of the bones of this skeleton might be found by judicious excavation of the low land on the opposite side of the highway. Our attention is so often directed to the finding of mastodon bones in this State that I have undertaken to bring together . in another part of this report, simply as a matter of record, a list of such discoveries made, so far as records show, within the boundaries of the State. This list may be imperfect, but it is a significant one. There appear on it entries of about 60 different finds of this kind; and, while the most complete of the skeletons have been found in the swamps of Orange county, the record shows that the remains have been also pretty freely distributed throughout the western part of the State. I have pointed out there that these occurrences for the most part. indi- cate that mastodons roamed the territory of New York prob- ably in such abundance as the buffalo roamed the western plains 40 years ago. It is not a matter of wonder that few complete skeletons are found, as these remains are located mostly close to the surface, and such parts as were left exposed to the action of the air have naturally crumbled, while still other parts may have been destroyed by rodents or through other organic agencies. And it is also noted that the location of these bodies, not far from the surface and, in the vast ma- jority of cases, on Swamps deposited on relatively recent river terraces or lake beaches, goes to indicate that the interval of — time separating the present from the day of the mastodon is not great; that these animals pertain to a late stage in post- elacial history and were doubtless contemporaneous with man, as is specially indicated by the Attica mastodon excavated ny the writer in 1887. | REPORT OF THE STATE PALEONTOLOGIST 1902 865 Other field work. Mr Richard F. Morgan has made for us some collections in the Marcellus limestone, temporarily ex- posed at Stony point south of Buffalo, at a time when such collections were much needed. Mr H. S. Mattimore has also collected to some extent in the Black river limestone in Jefferson county. Office work Memoir on the Guelph fauna in the State of New York. Ref- erence is made on a previous page to the field work done during the past season with reference to these investigations. We have brought together in the memoir now in press a detailed account of this fauna, which, in New York, has risen to the very considerable representation of 70 species. It has been shown that this characteristic Guelph fauna, constituting vir- tually a new element in the Paleozoic limits of the State, entered from the west, penetrating as far east during the period of the deposition of the Niagaran dolomites as eastern Orleans county, and then retreated, reappearing after an interval in which some 30 to 40 feet of Niagaran dolomites had been deposited, and in the second invasion reaching as far east as the vicinity of Rochester. This second appearance of the fauna was less com- plete in species than the first, and its horizon lies at or very close to the summit of the dolomites, making thus a phenomenon pertaining to the closing stage of the dolomite episode. The little cluster of fossils of this fauna, which were reported as long ago as 1848 by Professor Hall from the Erie canal at Newark, Wayne co., a locality from which nothing more has ever been obtained, seems to have come from a still higher horizon within the basal deposits of the Salina shales, where, under - unfavorable conditions, the impoverished representation of the Guelph fauna made its final appearance. The consideration of this fauna, which is illustrated by 21 quarto plates, involves the analysis and discussion of the nature of the sea and of the sediments of the Guelph period of time; and we have shown with reasonable conclusiveness that these deposits are ascrib- able to coral reef formations occurring in an inclosed and shal- lowing sea, which was gradually approaching the conditions essential for the free precipitation of salt and gypsum, such as prevailed during the succeeding Salina stage. The sea was one 866 NEW YORK STATE MUSEUM comparable in many respects to the present condition of the Red sea, receiving comparatively little fresh-water drainage with its exit to the ocean body constricted, and its shore lines dotted with coral reefs, on which flourished in immense pro- fusion a great variety of forms of invertebrate organic life. Memoir on the fauna of the Naples beds. In the 16th annual report of the state geologist, I published an account of the Cephalopoda of the Naples fauna, in which the great abund- ance of heretofore undescribed species was made known. Next in interest to the cephalopod element of this fauna come the lamellibranchs, and of these nearly 70 species are now described in the memoir in hand, together with such species of gastropod and other mollusca as appear in the fauna. This remarkable contribution of new facts is by no means the sole justification for the presentation of the Naples fauna. It is well recognized that this organic congeries, known as the fauna of Manticoceras intumescens, is one of the most persistent and widespread of the zones of organic life known in geologic history. Its affiliations with other manifesta- tions of this zone have been pointed out in a general way by the writer on other occasions, but this presentation affords the first opportunity for a close analysis of the elements of the fauna and their comparison with their manifestations in other countries. These investigations have led further to a clear con- ception of the conditions under which the fauna flourished and of its relations to contemporaneous faunas within the State of New York, so that we are now able to derive a definite idea of the diversity of the geographic provinces which existed during Portage time. Of these we have frequently spoken, recognizing the fact that the Naples fauna or the western fauna of the Portage time was an invader from the west, but till now we have not seen clearly that this western or Naples fauna is itself divided into two geographic elements, one of which pene- trated farther east than the other. So that in Portage time we find that the eastern part of the State was occupied by a brackish or estuarine fauna represented by the Oneonta beds, the central region by the autochthonic Ithaca fauna derived from its immediate predecessor on the ground, the Hamilton fauna, while the western province, which we have termed the REPORT OF THE STATE PALEONTOLOGIST 1902 867 Genesee, occupied as a whole by the Naples fauna, was divisible into two subprovinces, the eastern or Naples and the western or Chautauqua. This memoir, it is hoped, will be printed during the current year and will be accompanied by about 20 quarto plates of illustration. . Catalogue of type specimens of Paleozoic fossils. A year ago I announced that the compilation of this catalogue had been com- pleted and the printing begun. Printing has continued without interruption during the past year, and at the date of writing there are 650 pages completed. The work goes slowly, as it is one requiring great accuracy of treatment, but I hope to report the catalogue published before another year. With com- plete entries of all the type specimens now in our possession, the number of which constantly grows, the book will not fall far below 1000 pages and will include considerably over 5000 en- tries. Concurrent with the work of printing this catalogue, the labeling and ticketing of the types has been carried forward to correspond with the numbering in the catalogue itself. This has involved bringing most of our type specimens together in our rooms in the State Hall, though some part of them are left in their places in the exhibition collection in Geological Hall, because of the difficulty of replacing them with other specimens _ without disturbing the arrangement there. The work of arrang- ing the types has been largely in the hands of Mr Mattimore and has been carried out with much care. | The crustaceans from the Salina (Pittsford) shales in Monroe county. In my first report I noted the fact that the museum had by purchase come into the possession of a unique collection of heretofore unknown fossils from a horizon at the base of the Salina shales, also unknown till that time. This is a thin layer of black shales made known by excavations in the Erie canal near Pittsford in the year 1897. So distinctive is the character of this formation and its fauna that we are distinguishing the layer by the term Pittsford shale. Mr C. J. Sarle, of Rochester, was the discoverer of the horizon and the fossils. When Mr Sarle’s collec- tion passed into the hands of the State, he was promised an oppor- tunity to publish with us an account of the peculiar eurypterid 868 NEW YORK STATH MUSEUM Crustacea contained in this fauna, and this very interesting publication is presented with this report. Mr Sarle has spent some weeks here, engaged under my direc- tion in prosecuting his studies, and the objects which he first brings to public notice will be esteemed of much interest to all students of these ancient and primitive crustaceans, specially the proposed new genus Hughmilleria, which is intermediate between the well known genera Eurypterus and Pterygotus. T'wo years ago the writer described some of the phyllocarid Crustacea from these Salina shales and one form of the strange genus Pseudoniscus, so that now the entire list of crustaceans from the shales is as follows: Emmelezoe decora Clarke Ceratiocaris (Limnocaris) praecedens Clarke Pseudoniscus roosevelti Clarke Kurypterus pittsfordensis Sarle Hughmilleria socialis Sarle H. socialis var. robusta Sarle Pterygotus monroensis Sarle Publications During the past year the publications of the department have been two in number, Bulletins 49 and 52. The former contained various brief paleontologic papers as follows: Trenton Conglomerate of Rysedorph Hill and its Fauna, by Rudolf Ruedemann. Marcellus Limestones of Central and Western New York and their Fauna, by John M. Clarke. Marcellus Limestones of Lancaster, Erie co., by Elvira Wool New Agelacrinites, by John M. Clarke. Amnigenia as an Indicator of Fresh Water Deposits during the Devonic of New York, Ireland and the Rhineland, by John M. Clarke. The latter comprised papers on the following topics: Contact Lines of Upper Siluric Formations on the Brockport and Medina Quadrangles, by J. M. Clarke, Rudolf Ruedemann and D. D. Luther. REPORT OF THE STATE PALEONTOLOGIST 1902 869 Paleontologic Results of the Areal Survey of the Olean Quad- rangle, by John M. Clarke. Potsdam Sandstone of the Lake Champlain Basin, by Gilbert van Ingen. Graptolite Facies of the Beekmantown Formation in Rensse- laer county, N. Y., by Rudolf Ruedemann. Growth and Development of Goniograptus thureaui McCoy, by Rudolf Ruedemann. Fossil Alga from the Chemung of New York, by David White. A new Genus of Paleozoic Brachiopods, Eunoa, by John M. Clarke. Stratigraphic Value of the Portage Sandstone, by D. D. Luther. Paleozoic Seas and Barriers in eastern North America, by E. O. Ulrich and Charles Schuchert. Indigene and Alien Faunas of the New York Devonie, by John M. Clarke. The succession of faunas on the Salamanca quadrangle. The col- lections which had been made in the field during the survey of the Salamanca area were carefully studied and determined for use in the delineation of the formations on the map. These determinations were made in this office by Mr Charles Butts, | who was occupied therewith during the early part of the year. Cooperation with the state engineer and surveyor. By an ar- rangement made with the state engineer and surveyor, we have been able to avail ourselves of the services of Gilbert van Ingen, formerly instructor in geology at Columbia University. Mr van Ingen gives one half of his time to the official named and the other half is given to duties connected with this office. He has therefore been engaged in prosecuting investigations which he had previously begun on the Potsdam sandstone and the fauna of the Beekmantown limestone. This arrangement is a tem- porary one, and we can not hope for its continuance after the expiration of April next. . The areal and paleontologic maps of the Canandaigua and Naples quadrangles. In my last report I noted that these maps had been essentially completed, and that we have here endeavored to establish a more detailed subdivision of the formations than has before been attempted. During the past year these maps have been carefully revised and corrected, and some time was 870 NEW YORK STATE MUSEUM | spent by D. D. Luther in the office on this work. They are now in the hands of the engraver, and it is hoped that they will soon be available. The fauna of the pyrite layer at the horizon of the Tully limestone. I reported last year that an investigation of this subject was under way, and I am gratified to be able to incorporate the results of this work in this report. The work has been carried forward at my suggestion by Dr F. B. Loomis, assistant pro- fessor of biology at Amherst College. Its interest lies in the fact that we have here to deal with conditions influencing or- ganic associations at the sea bottom, which can be interpreted only by actual experiment or from the most careful results of recent investigations on the varying conditions in existing bodies of salt water. Certain factors prevailing during Paleozoic time have brought about a segregation of iron sulfid in the sea water, which has deposited itself in an almost continuous sheet over a distance of 100 miles along the edge from : Canandaigua lake to Lake Erie. With it are involved multitudes of . organic remains, all of them of extraordinarily diminutive size and yet, as Dr Loomis has shown, representing ar- rested and primitive phases of the profuse fauna which occu- pied the ground before these peculiar conditions set in. This — important fact being determined, namely that the fossils are only modified stages or conditions of the organisms which pre- vailed in that sea, the theorem is to demonstrate the character of the sea which could produce such a deposit. It has been usual to regard black bituminous shales, which generally carry large quantities of such pyrite deposits, as indicative of shallow or foul waters where decomposition has gone on with so much freedom as to produce directly much carbonate of iron and thus indirectly the sulfid. It is not however certain that we are cor- rect in a conclusion of this kind, as recent studies of confined bodies of sea water, for example the Black sea, have indicated © that separation of the sulfid is largely due to bacteria acting on the animal remains, but this is a process which takes place in the great depths where the bottom is covered with black mud, so that by comparison, such pyrite deposits, together with the - black bituminous shales with which they are usually associated, REPORT OF THE STATE PALEONTOLOGIST 1902 871 indicate a greater rather than a lessened depth of the sea. It is an illustration of one of the constantly increasing instances in which the paleontologist must be armed for the proper inter- pretation of ancient physiography with the growing volume of facts derived from the study of existing conditions. Personnel of the staff The permanent staff of this department has been changed during the year only in consequence of the death of George B. Simpson, draftsman; slight alterations have been made in the title of two of the assistants. The staff is as follows: R. Ruedemann, assistant state paleontologist D. D. Luther, field assistant George S. Barkentin, draftsman Philip Ast, lithographer Jacob Van Deloo, clerk H. S. Mattimore, preparator Martin Sheehy, machinist The following men have been temporarily engaged in the work of the department: Prof. Charles Butts, on the fossils of the Salamanca quadrangle; | Prof. A. W. Grabau, on the survey of Becraft mountain; Gilbert van Ingen, on various special topics as above stated; C. A. Hartnagel, on the study of the Cobleskill limestone and its fauna; | Myron L. Fuller and F. G. Clapp, of the United States Geo- logical Survey, in field work on the Elmira quadrangle. W.S. Barkentin, Ruth Holden and Mary M. Mitchell have also assisted with the work of illustration. Respectfully submitted JOHN M. CLARKE State Paleontologist Oct. 1, 1902 872 NEW YORK STATE MUSEUM PHILIP AST 1839-1903 With sincere sorrow I chronicle the death, May 8, 1903, of Philip Ast, who has been engaged in the work of this depart- ment for a period of more than 32 years. Mr Ast was of German birth and his early training was that of the Latin school and gymnasium of his home town in Bavaria. At the age of 16 he entered the Bavarian army and served as an officer therein in the War of 1866 between Prussia and Austria. In 1870 he came to America. Mr Ast had a keen artistic sense and remarkable calligraphic facility but in what was to be the work of his life he had had neither experience nor knowledge. On his arrival in New York he secured employ- ment with the well known lithographic establishment of Julius Bien & Co. and so successful were his first attempts there that when Prof. James Hall, needing a lithographer for the execu- tion of the plates of the Palaeontology of New York, applied to Mr Bien, Mr Ast was sent to Albany to take up this work though his experience was then of but a few weeks’ standing. Free from the usual crudities of inexperience his efforts were from the start successful and demonstrated not merely an apti- tude but a genius for the work. His activity in this career which has highly distinguished the illustrative work of this institution, began Ap. 1, 1871. The hundreds of lithographic plates of scientific objects executed by him remain as a record of his accomplishments, in the production of which he attained an adeptness and excellence which has never been elsewhere achieved in this country and few European workers have equaled his results for accuracy of delineation, perfection of finish and effect. His work raised the plates of the Palaeontology of New York to models of lithographic execution and exactitude. An artist on stone is at the mercy of the printer, and some- times a printer not over expert or none too conscientious has qualified the appearance of the imprints in a degree mortifying to the proper pride of the artist, but every lithographer comes to look with a sort of fatalistic toleration on such loss of the REPORT OF THE STATE PALEONTOLOGIST 1902 873 more delicate beauties of his achievement. It is right to say that these finer results of Mr Ast’s workmanship were never reproduced, were always sacrificed in some degree and their real beauties were known only to those who saw the stones before they left his hands. Mr Ast was a man of keen interests and intelligent apprecia- tions, kindly, true, loyal and generous. His life work was well done, and ended in his prime without a shade of departure from his standard. To such a servant, science in the State of New York owes no small debt. J. M. C. 874 NEW YORK STATH MUSEUM APPENDIX 1 ACCESSIONS I herewith submit the list of accessions to the collections made during the year, and, in continuation of the record of fossilifer- ous localities, parts of which have been communicated in the last three reports, the additional localities entered during the course of the past year’s work [Appendix 2]. The additions to the paleontologic collections have been by donation, purchase and collection. A detailed statement of these acquisitions is given herewith. Donations Wilson, J. D., Syracuse Gyroceras transversum Macrochilina onondagensis Mesothyra? Agoniatite limestone, Manlius Dakin, G. A., Syracuse Gomphoceras sp.? Agoniatite limestone, Manlius Wood, Elvira, Waltham Mass. Fossils from the Stafford limestone, Laneaster, Erie co. Onychochilus nitidulus Lunulicardium fragile Leptodesma marcellense Chonetes scitulus Camarotoechia prolifica? C. pauciplicata Wood Grant, C. C., Hamilton Ont. | Fossils from the Niagaran at Hamilton Fossils from the Clinton at Hamilton Barry, S. F., Sup’t Penrhyn Slate Co., Middle Granville Four large slabs bearing 69 specimens of Dactyloidites bulbosus from the Lower Cambric, Middle Granville pot more pp by (type) (hypotype) (hypotypes) (hypotypes) (hypotypes) (hypotype) (types) REPORT OF THE STATE PALEONTOLOGIST 1902 875 St John, Edward P., Hartford Ct. Coral from the Lower Chemung, Prattsburg 1 Udden, J. A., Rock Island Ill. Sponge from the Lower Carboniferous, Henton, Mills co. Ia. 1 Total by donation 92 (8 hypotypes, 3 types) Purchases Dolbel, A. F., Grande Gréve Que. Three barrels of Grande Gréve lime- stone fossils 900 Kranz, F., Bonn, Germany Fossil parasites | 14 Woodward, A. S. and Sherborn, C. D. Fossils from the Tilestones of Ludlow Eng. 215 Hartley, Frank, Cumberland Md. Fossils from the lowest horizon of the Hamilton group on Williams road near Cumberland Md. 150 Calder, Donald, Thurso, Scotland Old Red sandstone fiags, Thurso 20 Rae, John, Stromness, Orkney islands Old Red sandstone flags, Sandwick 19 Total by purchase 1318 ; Collections The paleontologist Old Red sandstone, Cromarty, Scotland 55 Old Red sandstone flags, Stromness, Orkney il Ruedemann, R. Cambric graptolites, sponges and brachi- opods at Schaghticoke 1650 Trenton fossils, Schuylerville 20 Cambric-Utica fossils collected in map- ping Cohoes sheet 450 876 NEW YORK STATE MUSEUM Ruedemann, R. and Luther, D. D. Fossils from the Guelph dolomites at Shelby 750 Luther, D. D. Fossils from Naples shales, Naples 78 Lower Chemung shales 35 Salina shales, Pittsford 20 Portage fossils from Erie and Chau- tauqua counties 172 Guelph fossils from Shelby 150 Mattimore, H. S. and Hartnagel, C. A. Fossils from the Upper Devonic out- crops on Elmira quadrangle 1200 Hartnagel, C. A. Collections from the Cobleskill limestone in Otsego, Schoharie and Ulster counties 1190 van Ingen, G. Lower Cambric, Middle Granville 20 Total by collection 6391 Total accessions 7801 | (3 types, 8 hy- potypes) REPORT OF THE STATE PALEONTOLOGIST 1902 8717 APPENDIX 2 NEW ENTRIES ON GENERAL RECORD OF LOCALITIES OF AMERICAN PALEOZOIC FOSSILS BELONGING TO THE STATE MUSEUM ALPHABETIC LIST OF LOCALITIES Albany (Albany co.), 3205, 3221 Angola (Erie co.), 3098, 3099, 3100, 3101, 3102 Bath (Rensselaer co.), 3220 Big Sister creek (Erie co.), 3108, 3104 Bird creek (Chemung co.), 3177. Bradnor Hill, Kingston Eng., 112 (yellow ticket) Bradnor Lane, Kingston Eng., 120 (yellow ticket) Brindgwood Chase Eng., 118, 114 (yellow ticket) Brunswick (Rensselaer co.), 3213 Carr hill (Chemung co.), 3164 Catlin (Chemung co.), 3168, 3169, 3170 Christian hollow (Chemung co.), 3171, 3172, 3173, 3174 Corning (Steuben co.), 3142, 3143 Deep kill (Rensselaer co.), 3206, 3207, 3211, 3223 Downton, England, 121 (yellow ticket) East Corning (Steuben co.), 3165, 3167, 3190, 3191 Highteen Mile creek (Erie co.), 3103, 3104 Elmira (Chemung co.), 3147, 3148, 3149, 3155, 3156, 3171, 3172, 3186, 3187, 3188, 3189, 3192, 31938, 3194, 3198 Farnham creek (Erie co.), 3101 Faulkner’s ravine (Chautauqua co.), 3105, 3106, 3109 Fitch bridge (Chemung co.), 3146 Forestville (Chautauqua co.), 3113, 3114, 3115, 3116, 3117, 3118, 3120, 3121 Fruing’s Que., 3094 Grant Hollow (Rensselaer co.), 3216 Hamilton Ont., 3127, 3128 Hargeest Mill, Kingston Eng., 122 (yellow ticket) Hawley hill (Chemung co.), 3149 Hendy creek (Chemung co.), 3186, 3187, 3188, 3189 Horseheads (Chemung co.), 3152, 3153, 3154, 3155, 3156. 3163 Johnson hollow (Chemung co.), 3130, 3132, 3139, 3199, 3200, 3201 878 NEW YORK STATE MUSEUM Johnsonville (Rensselaer co.), 8222, 3225 Keeseville (Essex co.), 3095 | Lansingburg (Rensselaer co.), 3202, 3204, 3208, 3210, 3213, 3228 Latty brook (Chemung co.), 3155, 3156 Lower Pine Valley (Chemung co.), 3130, 3181, 3132, 3139, 3199 Ludford Eng., 111, 117 (yellow ticket) Ludford Lane Eng., 118, 123 (yellow ticket) Ludlow Eng., 108, 109, 115, 119, 121 (yellow ticket) Madison creek (Chemung co.), 3168, 3169 Mechanieville (Saratoga co.), 3203 Melrose (Rensselaer co.), 3209, 3217, 3218, 3223 Menands (Albany co.), 3221 Millport (Chemung co.), 3133 Mt Zoar (Chemung co.), 3192, 3193, 3194, 3195, 3196 Mudlick creek (Chemung ¢o.), 3197 Nashville (Chautauqua co.), 3106, 3109 Northeast Pa., 3107 North Elmira (Chemung co.), 3157, 3158, 3159, 3160 North Evans (Erie co.), 3103, 3104 Oak Orchard creek (Orleans co.), 3122, 3124, 3125 Onibury Eng., 116 (yellow ticket) Pike creek (Erie co.), 3096, 3097 Pine City (Chemung co.), 3178, 3179, 3180, 3181, 3182, 31838, 3184, 3185, 3197, 3198 Pine Valley (Chemung co.), 3135, 3136, 3187, 31388, 3150, 3151, 3161, 3162, 3163, 3164 Post Creek (Chemung co.), 3140, 3141, 3144, 3145 Prospect hill (Essex co.), 3095 Raymertown (Rensselaer co.), 3218 Rosstown (Chemung co.), 3173, 3174, 3175, 3176 Schaghticoke (Rensselaer co.), 3229, 3230 Schuylerville (Saratoga co.), 3212 Seeley creek (Chemung co.), 3185 Shelby (Orleans co.), 3122, 3128, 3124, 3125 Silver creek (Chautauqua co.), 3109 Shumla (Chautauqua co.), 3109 Smith’s Mills (Chautauqua co.), 3105, 3109, 3110, 3111, 3112 Southport (Chenango co.), 3198 Speigletown (Rensselaer co.), 3210, 3217, 3218, 3228 REPORT OF THE STATE PALEONTOLOGIST 1902 879 Terry’s ravine (Chautauqua co.), 3116 Tomhannock (Rensselaer co.), 3222, 3224, 3226, 3227 Tomhannock creek (Rensselaer co.), 3214, 3215 Troy (Rensselaer co.), 3220, 3221 Walnut creek gorge (Chautauqua co,), 3117, 3118, 3119 Ward’s lane (Albany co.), 3205 Wells (Chemung co.), 3177 Whitecliffe Eng., 110 (yellow ticket) Wilson’s creek (Rensselaer co.), 3210 Winfield creek (Chemung co.), 3165, 3166 Winona Ont., 3129 NEW YORK LOCALITIES ACCORDING TO COUNTIES (Names in italic are new to the record) Albany co. Millport Albany Mt Zoar Menands Mudlick creek Ward’s lane North Elmira Chautauqua co. Christian hollow Elmira Fitch bridge Hawley hill Hendy creek Horseheads Johnson hollow Latty brook Madison creek Pine City Faulkner’s ravine : ! Pine Valley Forestville 4 Post Creek Nashville Sainile Rosstown Silver creek Be encneey Smith’s Mills Southport Terry’s ravine ee Walnut creek gorge Winfield creek Chemung co. Erie co. Bird creek Angola Carr hill Big Sister creek Catlin Eighteen Mile creek Farnham creek North Evans Pike creek Essex co. Keeseville Prospect hill Orleans co. Oak Orchard creek Shelby NEW YORK STATE MUSEUM Rensselaer co. Tomhannock creek Bath Troy Brunswick Wilson’s creek Deep kill Saratoga co. Grant Hollow Mechanicville Johnsonville Schuylerville Lansingburg Steuben co. Melrose Corning Raymertown East Corning Schaghticoke Washington co. Speigletown Middle Granville Tomhannock INDEX TO FORMATIONS Cambric, 8228, 3229, 3230 Georgian, 3126, 3210, 3216 Lower Siluric, 3211 Trenton limestone, 3095, 3129, 3202, 3208, 3212, 3218, 3214, 3215, S217, S218, o29, 3222, 32240 3295, 3226 3297 - Normans kill shale, 3202, 3208, 3212, 3213, 3214, 3215, 3217, 3218, 3219, 8222, 3224, 3225, 3226, 3227 Utica shale, 3208, 3204, 3205, 3209, 3220, 3221, 3223 Lorraine, 3206, 3207 Clinton beds, 3128 Niagaran, 3127 Lockport limestone, 3124 Guelph formation, 3122, 3128, 3124, 3125 Devonic (Grande Gréve limestone), 3094 : | Portage beds, 3096, 3097, 3098, 3099, 3100, 3101, 3102, 3103, 3104, 3110, 3111, 3112, 3115, 3116, 3118 Cashaqua shales, 3096, 3103 Ithaca beds, 3118, 3114, 3117, 3119 Chemung beds, 3105, 3106, 3107, 3108, 3109, 3113, 3114, 3117, 3119, 3120, 3121, 3180, 3131, 3132, 3183, 3134, 3135, 3136, 31387, 3138, 3139, 3140, 3141, 3142, 3148, 3144, 3145, 3146, 3147, 3148, 3149, 3150, 3151, 3152, 3153, 3154, 3155, 3156, 3157, 3158, 3159, 3160, 3161, 3162, 3163, 3164, 3165, 3166, 3167, 3168, 3169, 3170, 3171, 3172, 3173, 3174, 3175, 3176, 3177, 3178, 3179, 3180, 3181, 3182, 3183, 3184, 3185, 3186, 3187, 3188, 3189, 3190, 3191, 3192, 3193, REPORT OF THE STATE PALEONTOLOGIST 1902 881 3194, 3195, 3196, 3197, 3198, 3199, 3200?, 3201 Laona sandstones, 3105, 3106, 3109 3094 3095 3096 3097 3098 3099 3100 3101 3102 3103 3104 , 3105 3106 RECORD OF LOCALITIES Grande Gréve limestone. Fruing’s, Quebec, Can. A. F. Dolbel, collector. 1902. Trenton limestone. Loose block at roadside west side of Prospect hill, 144 miles southeast of Keeseville, Essex co. N. Y. Station 150 C3. G. van Ingen, collector. 1901. Portage (Cashaqua) shales. Pike creek, Erie co. Top of Cashaqua shales. D. D. Luther, collector. 1902. Portage shales. Lower black band near mouth of Pike creek, Erie co. D. D. Luther, collector. 1902. Portage shales. Angola, Erie co.; lake shore. Horizon, top of second black band. D. D. Luther, collector. 1902. Portage shales. Angola; under Lake Shore railroad bridge. Horizon of big goniatites. D. D. Luther, col- lector. 1902. Portage shales. Base of second gray band. Angola. D. D. Luther, collector. 1902. Portage shales. Angola; lake shore, mouth of Farnham ereek. D. D. Luther, collector. 1902. Portage shales. Angola. Big Sister creek near mill; 25 feet above top of second black band. D. D. Luther, collector. 1902. Portage (Cashaqua) shales. Eighteen Mile Creek; North Evans. Mostly from concretions. I). D. Luther, col- Jector. 1902. Portage Shales. Eighteen Mile creek; North Evans. Base of second black band. D. D. Luther, collector. 1902. Chemung beds. Faulkner’s ravine 214 miles south of Smith’s Mills. From the (Laona) sandstones. D. D. Luther, collector. 1902. Chemung beds. Faulkner’s ravine, 114 miles north of Nashville, Chautauqua co. The (Laona) sandstones. D. D. Luther, collector. 1902. 882 SLOT 3108 3109 3110 3111 3112 3113 3114 3115 3116 3117 3118 3119 NEW YORK STATE MUSEUM Chemung beds. Sixteen Mile creek; Northeast Pa., From an exposure along the brook that flows through the southern part of village, at a point about 14 of a mile from Lake Erie and 25 feet above lake level. Sur- face of flags. D. D. Luther, collector. 1902. Chemung beds. In the gorge at Shumla, Chautauqua co. A few Orthis and Productella occur in several layers. D. D. Luther, collector. 1902. Chemung beds. Smith’s Mills, Chautauqua co., 3 miles south of, on road to Nashville. Faulkner’s ravine; branch of Silver creek. The (Laona) sandstone. D. D. Luther, collector. 1902. Portage. Roadside 114 miles west of Smith’s Mills. D. D. Luther, collector. 1902. Portage. Ravine 14 mile west of Smith’s Mills. D. D. Luther, collector. 1902. Portage. Smith’s Mills; 15 feet below the row of con- cretions in ravine east of hotel. D. D. Luther, collector. 1902. Chemung or Ithaca beds. Ravine 14 mile east of Forest- ville, Chautauqua co.; about 100 feet above sandstone, second fossiliferous layer above sandstone. D. D. dane collector. 1902. Chemung or Ithaca beds. Ravine east of Forestville. From thin calcareous layer about 50 feet above sand- stone. D. D. Luther, collector. 1902. Portage. Forestville; below railroad bridge. D. D. Luther, collector. 1902. | | : Portage. Forestville. Above railroad bridge and below mill; from concretions on Walnut creek gorge. D. D. Luther, collector. 1902. Chemung or Ithaca beds. Forestville; Terry’s ravine. From the sandstone at top of falls. D. D. Luther, col- lector. 1902. Portage. Forestville; Terry’s guily; 50 feet below sand- stone. D. D. Luther, collector. 1902. Chemung or Ithaca beds. Forestville; Terry’s ravine. Horizon of the sandstone. D. D. Luther, collector. 1902. REPORT OF THE STATE PALEONTOLOGIST 1902 883 3120 Chemung beds. Forestville. From the sandstone on Wal-— nut creek. D. D. Luther, collector. 1902. 3121 Chemung beds. Forestville. Small ravine in heart of village; about 50 feet above sandstone. D. D. Luther, collector. 1902. 3122 Lower Guelph dolomite. Oak Orchard creek, 14% mile south of Shelby. R. Ruedemann and D. D. Luther, collectors. 1902. 3123 Shaly limestone 8 to 10 feet above Lower Guelph dolo- mite. Shelby. D. D. Luther, collector. 1902. 3124 Lockport limestone below Upper Guelph dolomite along Oak Orchard creek, about 2 miles south of Shelby. R. Ruedemann and D. D. Luther, collectors. 1901 and 1902. ) 3125 Upper Guelph dolomite exposed along Oak Orchard creek about 2 miles south of Shelby. R. Ruedemann and D. D. Luther, collectors. 1901 and 1902. 8126 Georgian. Dactyloidites from black slate overlying the “flint” bed in the first quarry of the Penrhyn Slate Co.’s quarries at Middle Granville, Washington co. N. Y. Penrhyn Slate Co., Granville N. Y., donor and G. van Ingen, collector. 1902. 3127 Niagaran. Hamilton Ont. C. C. Grant, donor. 1902. 3128 Clinton beds. Hamilton Ont. C. ©. Grant, donor. 1902. 3129 Trenton drift. Winona Ont. C. C. Grant, donor. 1902. FOSSILS COLLECTED BY C. A. HARTNAGEL AND H. 8S. MATTIMORE IN AREA COVERED BY THE ELMIRA QUADRANGLE, CHEMUNG-AND STEUBEN countins, 1902. LocaLirty NumMBERS 3130-3201 INCLUSIVE 51380 Chemung beds. Johnson hollow, 34 mile northwest of Lower Pine Valley, Chemung co. (A! 1324 ft A. T.) 3131 Chemung beds. Johnson hollow; northeast escarpment of 1500 foot hill 34 of a mile northwest of Lower Pine Valley. (A? 1277 ft A. T.) 3132 Chemung beds. c t ig F F « 0 [ree VZZZZZT acess BLUE *GREEN SHALE Zi —| Z REO SHALE 6 Zz 3 Tm 1100 z PURPLE SHALE LIME STONE ASYLUM QUARRY FISH BEDS =] TANNER'S HILL 1400 QUARRY 13900 1200 = F, Wolf run east of Corydon; G, Warren Pa. Columnar sections: A, Genesee rock city; B, Mt Hermon-Flatiron; C, Knapp’s creek; D, Dennis well, Bradford; 8, Limestone; (the last after Randall) 1817 1830 1838 1866? 1885 1826 - REPORT OF THE STATE PALEONTOLOGIST 1902 931 Monroe county Rochester Some remains were found in Rochester, in a hollow or watercourse. De Kay. Nat. Hist. N.. Y.; Zool. 1842. pt 1, p. 103 Pittsford Tusk and one cervical vertebra. Bank.of Irondequoit ereek, 214 miles from Pittsford. J. A. Guernsey. Am... Jour. Sci. 1831. 19:358 Rochester Along Genesee valley canal on Sophia street. Tusk. bones of head, several ribs, vertebrae, tibia and part of pelvis. These were found in gravel covered by clay and loam, and above them a deposit of shell marl. They were placed in the State Museum. Hall. Geol. Fourth Dist. 1843. pp. 364 Rochester | A few remains at Mount Hope cemetery. HA. L. Ward Ontario county Seneca Excavated by Henry J. Peck on farm of Charles Greg- ory, where the bones had been discovered about 1882. : Found beneath marl and diatom earth, about 3 feet from the surface. Sixty-five bones were obtained, mostly ribs and vertebrae with one tusk, 9 feet on outer curve, and styloid 1 inch longer than in the Warren mastodon. The antler of an elk was also found [see pl. 2]. The bones are now in the collection of Amherst College. H. J. Peck Livingston county Geneseo One half mile east of Geneseo. Tusks, head and lower jaw with eight teeth, pelvis and many other bones. Jer. Van Rensselaer. Am. Jour. Sci. 1827. p. 381 Subsequent excavations were made by James Hall and Sir Charles Lyell, and fragments of bones were found mixed with marl! and fresh-water shells. 932 Date? Date? 1886 NEW YORK STATE MUSEUM | Nunda Ten bones and fragments, collected by Rev. Milton Waldo and presented by R. S. Fellows to Yale ve Museum. C. EH. Beecher Scottsburg | Twenty bones and fragments. F. H. Bradley and H: A. Green collectors. R. S. Fellows, donor. Yale University Museum. (C. EH. Beecher . Fowlerville Found in excavation on bank of the Genesee river, 80 feet above the water. Three or four teeth, tusks and other bones which were badly broken. H. J. Peck 1835-40 Stafford Genesee coy 1841 1897 1877 1886 Tooth found beneath muck on clay and siti? Halt. Geol. Fourth Dist. 1843. p. 364 Leroy Tooth in bed of marl, 3 miles south of lene, Hail. Geol. Fourth Dist. 1843. p. 364 Batavia Two tusks, part of skull with teeth, several vertebrae and ribs. H. L. Ward Pike Wyoming county Tusks, part of skull, some vertebrae and foot bones. Now in the Letchworth Museum at Glen Iris, Portage - falls. Attica Small tusk, ribs and other bones found in digene trench on Genesee street, in unlaminated clay at a depth of 2 to 3 feet, overlaid by clayey muck and loam. Be neath these bones were found several pieces of charcoal. In another part of the same swamp, under 4 feet of muck and 1 foot below level of the bones, was found a con- — siderable quantity of charcoal with broken pottery. Clarke. N. Y. State Geol. 6th An. Rep’t. 1887. p. 34; 7th An. Rep’t in N. Y. State Mus. 41st An. Rep’t. 1888. p. 388 =. CO eee eee eee —_—_. + eee ee ee as REPORT OF THE STATE PALEONTOLOGIST 1902 933. Orleans county 1820 (?) Holley Tooth found in excavation for Erie canal. Hall. Geol. Fourth Dist. 1843. p. 364 Niagara county Date? Niagara Falls Tooth in fine gravel and loam containing fresh-water shells. Hall. Geol. Fourth Dist. 1843. p. 364 Found in digging a mill race on Goat island, 12 or 13 feet below the surface. De Kay. Nat. Hist. N. Y.; Zool.. 1842. pt1, p. 104 | Chautauqua county 1884 Jamestown Part of jaw with two teeth. Found by John Hazeltine in muck “a little below the present level” of Chautauqua lake outlet. Am. Jour. Sci. 1835. 27:166 Associated with bones of elk. De Kay. . Nat. Hist. N. Y.. Zool.; 1842. pti, p. 120 1902 Westfield On property of Mrs Alice Peacock, alongside Nickel Plate Railroad. The bones lay on pavement of heavy boulders and under several feet of black clayey muck. They consisted of 1 tusk (6 feet, 2 inches, and highly curved), 17 ribs, 8 pelvic and lumbar vertebrae, patella. and parts of scapula and pelvis. Clarke Cattaraugus county Date? Hinsdale Tusk with remains of deer (elk?) 16 feet beneath sur- face in gravel and sand. Hall. Geol. Fourth Dist. 1843. p. 364 1870 (?) Near Ithaca Five teeth and many fragmentary bones “in a deposit of modified drift.” “The teeth indicate the existence of two or more individuals.” B. G. Wilder. Am. Jour. Sci.. 1871. 2:58 | Tompkins county THE CAMBRIC DICTYONEMA FAUNA IN THE SLATE BELT OF EASTERN NEW YORK BY RUDOLF RUEDEMANN ~ ‘Introduction With the progress of the investigation of the thick masses of shales, slates and flags, extending to the east and south of the great St Lawrence and Hudson river valleys from Gaspé to southern New York, or to the east of “ Logan’s line,” it becomes more and more apparent, that Lapworth exhibited a prophet’s intuition in predicting many years ago, that this mass, generally lumped together as Quebec and Hudson river groups, would be found to represent, formation by formation, the more or less ¢al- careous series to the west and north of that line, from the Pots- dam below to the Lorraine above. In the last report of the state paleontologist the writer an- nounced the discovery of three different graptolite zones, ex- posed at the Deep kill in Rensselaer county, which represent the Phyllograptus-Tetragraptus shales of northern Europe and Canada. From their identification with the Point Levis shales of Canada and by correlation with the corresponding zones of Europe, they are placed in the lowest Lower Siluric, and con- sidered as representing the shaly development of the Beekman- town limestone and perhaps also of the Chazy limestone. The continuation of the investigation of the slates of Rensse- laer county has this year led, at Schaghticoke on the Hoosick river, to the finding of an outcrop of slates which contain a fauna known from the northeast of this continent and from Europe, and there considered as marking the closing stage of Cambric time. A very large quantity of excellently preserved material has been secured, the graptolitic part of which will be . described in a forthcoming memoir. In this report, it is pro- posed to discuss only the geologic aspect of the discovery. Description of locality and beds The outcrop extends from the bridge of the Mechanicville- Johnsonville branch of the Fitchburg railroad, on both sides of the gorge for about one half mile. The river is forced, in this Soqv]s BIIdUOAQOICT o1aquaeg teddy Jo ommsodxm +X ‘N oYOor Sey, yW AOALL OISOOFT OY} JO sT[V] JoMO'T I 93¥1d REPORT OF THE STATE PALEONTOLOGIST 1902 935 distance, to plunge three times over precipices caused by the rocks in question and to form the waterfalls, a part of whose great water power is utilized now in the mills of Schaghticoke. The outcrop is totally isolated, there being an interruption of three quarters of a mile to the outcrops farther above the river, near the powder mills of Valley Falls, the interval being filled by drift. Likewise the Schaghticoke beds are separated by a drift-filled interval from the masses of shales and heavy banks of “ Hudson grit,” exposed a little farther down the river. There is no doubt that the latter mass, which contains graptolites of the upper half of the Lower Siluric, is separated from the beds at Schaghticoke by a great fault, probably the same which farther south, for instance at Rensselaer, separates the Cambric and Trenton shales. The Schaghticoke slates disappear also north and south of the river banks under great drift masses and do not reappear for considerable distances. It is however very probable or almost certain that they represent a continuation of the belt of Cambric rocks (shales, slates, quartzite and limestones) which are well exposed on the hills east of Troy and have become well known by Ford’s discoveries of fossils. This belt has been traced and mapped by Walcott,! as extending as far as the Deep kill and been found by the writer to continue in fossilifer- ous beds still farther north, east and northeast of Melrose to within a few miles of the outcrop at Schaghticoke. As the lat- ter lies also in the direct strike of these Cambric beds, it is fairly to be concluded that it is a northward continuation of that belt. ; The Cambric beds of the slate belt of eastern New York have thus far furnished only fossils of the Lower Cambric or Georgian formation. The Dictyonema beds will, as we may anticipate, be shown to be equivalent to the highest Upper Cambric beds and may, hence, in a general way be said to represent part of the off-shore deposits of the Potsdam or Upper Cambric formation. The entire mass of rocks, exposed for about half a mile in the gorge of the Hoosic river at Schaghticoke, consists of very fine bedded, black and prevailing dull greenish to olive silicious and 1Am. Jour. Sci. 1888. v. 35, pl. 3. 936 NEW YORK STATE MUSEUM argillaceous slates with interealations of thin limestone beds. The latter, consisting of hard gray, very fine grained limestone, are but about 1 inch thick and separated by black carbonaceous, argillaceous shales. These alternations of limestone bands and black, relatively soft shales, are well shown on plates 2 and 3. On plate 2 also the beds of green and black slates appear dis- tinctly by their different shades, and the thin bedding can be noticed. The whole terrane, which by the width of the outcrop might be taken to represent a considerable thickness, is appar- ently nothing but a manifold repetition of the same series of beds in small, closely packed, and in all conceivable ways dis- torted folds. The latter appear distinctly on plate 3, which shows a part of the north bank of the river. The lithologic similarity of the Schaghticoke beds with those of the Deep kill, containing the Beekmantown-Chazy fauna, is very Striking; there occurring thin equally bedded, alternating, greenish and black slates and intercalated, thin, barren lime- stone bands. It is evident that there was no difference or break whatever in the physical conditions from the time of the depo- sition of these Cambric beds to that of the Lower Siluric beds; and the writer would not be surprised if in other localities they should be found to form a continuous series, as indeed is. strongly suggested by the results of Professor Dale’s investiga- tion of the lithologie and stratigraphic characters of the slate belt. Inclosed in these shales there have been found two different kinds of fossiliferous beds. The one is characterized by the occurrence of Dictyonema flabelliforme Hichwald, the other by that of Clonograptus proximatus Mat- thew. Both faunules have been observed in several places of _ the outcrop. This is partly due to a repetition of the same beds, but it is also obvious that neither of them is restricted to a single band, for one bed contained prevailing grown and half grown specimens of Dictyonema, while another bed, found a little farther down the river, carries nothing but the earliest — growth stages. Likewise, at least two different beds, containing the Clonograptus faunule, have been noticed. On account of the extremely disturbed condition of the beds, I have not been able to satisfy myself as to the relative position S9yBIS youlq puv Wools puv SpuBq sUOJSOUNT] UIYY oY} SMOYSZ AQ “N OYOoryYSeyo, ye sozeys vurouodqoiqg o1quieg soddgq jo oansodxy ce -338Ild REPORT OF THE STATE PALEONTOLOGIST 1902 937 of these faunules, but, as a few specimens of Dictyonema flabelliforme _ have been obtained from the Clonograptus beds, it is provisionally assumed that the faunules belong together as parts of a larger fauna and do not indicate sharply separated horizons. The author and Mr van Ingen were not successful in determin- ing the interval of rock between the two principal fossil beds or the thickness of the series of strata. All that could be established was that in one place the bed with Clonograptus is connected with a series of alternating black and olive-green slates, the latter char- acterized by worm tubes, which series has a thickness of 15 feet; that in another place a Clonograptus bed, presumably the same, is found overlying a series of 20 feet of like slates, which alternate with two series of thin, barren limestone bands [see pl. 2, which shows the lower series of limestone bands]. The principal Dictyonema horizon occurs in a 114 inch band of peculiar lith- ologic character, it being a soft, strongly ocher-spotted black mud shale, which has a highly developed and, for the paleontologist, very unfortunate system of contraction joints. This band is sepa- rated by about 10 feet of black or greenish slates from a series of thin limestone bands in about the same number as that men- tioned in connection with the Clonograptus bed. It is, hence, to be assumed that these two series of limestone layers are iden- tical, and that the series of rocks containing these beds is at least 30 feet thick, but most probably considerably more. The. fine black mud shale intercalated between the thin limestone bands, contains in another place great numbers of early growth stages of Dictyonema. | : The principal Dietyonema stratum has been found to contain these fossils in such numbers that all surfaces of the thinly bedded band are entirely covered by colonies of Dictyonema fla- belliforme Hichwald, forma typica (=D. sociale Sal- ter) and var. acadicum. On a slab of similar lithologic © character, lying loose on the bed, a valve of a Lingula or Lingu- lella, not sufficient for identification, was observed. The Clonograptus bands contain: Protospongia sp. . r Dictyonema flabelliforme Hichwald var. acadicum Matthew r 438 NEW YORK STATE MUSEUM Clonograptus proximatus Matthew (Staurograptus di- chotomus Hmimons) ec Clonograptus cf. milesi Hall Bryograptus lentus Matthew B. spinosus Matthew B. patens Matthew Acrotreta bisecta Matthew A. cf. belti (Davidson) Matthew Cet eer k teri (e) Mec) = ber) Notes on fossils The Protospongia occurs mostly in large spicules (or bundles of spicules), consisting of pyrite and limonite, the four branches measuring 10 mm and more. Walcott has figured spicules of smaller size but like form from the upper portion of the Olenel- lus zone in Washington county, N. Y., and pointed out their similarity with Prostospongia fenestrata Salter. Patches of sponge tissue have been found, composed of rhom- bic meshes of nearly half an inch wide and thereby reminding one of the gigantic form Palaeosaccus dawsoni Hinde, from the base of the Levis beds. As a large surface of the bed containing these sponges is accessible, a further exploitation of the same in another season will probably furnish sufficient material for an exact determination of the relation of this sponge to the form mentioned and to the species described by . Dawson from the Lower Levis beds at Little Metis. : Dictyonema flabelliforme Kichwald. There is some variation in the expression of the forms, and some of the varieties which have been recognized in other localities may also be discernible here. The great majority of the specimens however are clearly identical with Dictyonema flabelliforme KEichwald, forma typica, as it has been described by Kjerulf and Broégger. This is evinced by the rather open long meshes and the thin, slender dissepiments. Quite a number of forms possess rather fine meshes and may be comparable to the variety conferta ~ Linnarsson. The mutation norvegica, which is said by Broégger to lie in a higher level at Vakkeré, and which is char- acterized by small, short, angular meshes and thick connecting dissepiments, is not represented in the Schaghticoke fauna. The variety acadicum, which was recognized by Matthew IOAN OISOOF] JO YUVG YON “A “N opoorgyseyog 4v soyvjs vurouodzorql ouqureg teddy) oyy ul sploy € 21eId REPORT OF THE STATE PALEONTOLOGIST 1902 939 among the graptolites of the Cambric of the St John basin, is also present and recognizable by its small meshes and closely arranged thecae, 17 of which were counted in the space of 10 mm. But it must be added, that all these varieties occur inter- mingled in the same band and are connected by transitions. Clonograptus proximatus Matthew. We will not enter here on a description of the development of this species, nor on its interesting structure, but defer that part of the investigation to the description of the fauna. But it is here pertinent to point out that Emmons had evidently this form before him when he described his Staurograptus dichotomus This species of Emmons has, ever since its publication, been con- sidered with some distrust as a somewhat dubious form; and this with some justification, for Staurograptus is, compared with other graptolites, an odd looking fossil. Staurograptus has been recognized again by Lapworth in the Cape Rosier (Quebec) zone [loc. cit. p. 168] and is referred to as the “ dubious genus Staurograptus of Emmons.” Gurley cites the genus in his list without any comment, evidently because he did not know what to make of the form. Our large material of Clonograptus proximatus, which contains all growth stages from the sicula upward, includes also Emmons’s Staurograptus in unmistakable specimens and in great number. The peculiar branching of this form, which produces a cross in the center, instead of the crossbar (funicle) of the other Dicho- graptidae is the surest means of its recognition. Emmons’s Staurograptus is but a very early growth stage of Clonogr. proximatus Matthew. Emmons found his specimens in “the black Taconic shales of Rensselaer county, N. Y.” There occurs in the Clonograptus bed still another species of Clonograptus which is readily distinguished by its very loose branching and the small number of branches. This form is closely related to, if not identical with, Graptolithus milesi Hall.2. The habit of both species is alike, and the thecae fail to show any differences; Clonograptus milesi. has been found at Schaghticoke, though in much larger speci- 1 American Geology. 1855. 1:10), pl. 1, fig. 21. ® Geology of Vermont. 1861. ': 372; v. 2, pl. 13, fig. 2-4. 940 NEW YORK STATE MUSEUM mens than have been collected thus far, a difference which, however, is of no or little import. A differential character, however, which necessitates consideration lest hasty indentifi- cation might ensue, is the rapid twofold dichotomy in the Schaghticoke specimens, which, as in Clonograptus proximatus, leads to a crosswise branching in the center, while Clonograptus milesi possesses a “funicle” of considerable length. On the other hand, Clonogr. milesi is closely related to Clonograptus tenellus_ Linnarsson (sp.), a species which is found in Scania in beds intimately connected with the Dictyonema flabelliforme slate. In view of this relationship of Clonograptus milesi, it is important to note that that species does not belong to the Quebec group, as it is usually cited,’ but was derived from the slates at Georgia Vt. Hall says in regard to the provenience of his material: The specimen from which the figures of this species were de- rived, is part of a boulder of Georgia slate, picked up in Monk- ton by Henry Miles of Monkton . . . The boulder was probably derived from the Georgia slate, either in Georgia or St Albans. This citation is evidently not to be understood as meaning that Clonograptus milesi is a form of the Georgian or Lower Cambric formation; but it may be concluded with a fair degree of certainty that it came from Cambric slates lying somewhere near the top of the Cambric formation, and it is possible that this occurrence indicates the presence of another subzone in the Upper Cambric. . The discussion of the relations of the species of Bryograptus, cited in the list of the fossils of the Clonograptus bed, is reserved for the forthcoming description of the graptolite fauna of New York. Lingula. A brachial valve of a linguloid form, about 9 mm long; perhaps referable to Lingulella concinna, a species described by Matthew from the Dictyonema horizon of a McLeod brook, Boisdale, Cape Breton island. The Schaghticoke specimen appears more uniformly oval, but Mr Matthew’s speci- men is flattened out anteriorly and posteriorly, as appears from 1 Miller’s North American Geol. and Pal. p. 190. “KN a3ooryseyog, “TAL oISOOT] ‘ST[IUT UsTOOM MOTEq ‘SaqRIS BUIAUOAZOICT UL SPOT 2 i. yy) mee ‘ 4 uy i TAD REPORT OF THE STATH PALEONTOLOGIST 1902 941 his description, and may therefore have had a like shape. Our specimen is also somewhat larger than the Cape Breton form. Acrotreta bisecta Matthew. There also occur types of an Acro- treta in the Clonograptus bed, the pedicle valve of which has been noticed only in a very much compressed state but still ex- hibiting the subcentric pedicle perforation. The brachial valve possesses the long, high, posteriorly enlarged (or dividing? in many specimens) median ridge, extending the entire length of the shell, and also on the casi, at least one pair of the minute pits, features which Matthew considered characteristic of his species Acrotreta bisecta, a form from the Dictyonema shales at McLeod brook, Cape Breton.! As our form also agrees in general outline and dimensions with the Cape Breton species, it may well be considered as identical with the latter. Mat- thew has also recognized this species among the brachiopods collected in the Dictyonema shale at the Navy island, St John N. B. as the form which he had formerly described as Acro- treta baileyi. Acrotreta cf. belti (Davidson) Matthew. There occur small orbicular corneous brachiopod shells in the Clonograptus bed, which on account of their small size and compression offer con- siderable difficulty to a definite determination. The pedicle valve shows a small circular pedicle perforation, the brachial valve, which is well preserved, three narrow septa and pos- terior muscle impression, as one finds in Linnarssonia transversa Walcott. As the latter species has lately been reunited with Acrotreta by Walcott? this form is probably also referable to Acrotreta. It seems to us to be identical with the minute shells found by Matthew in the Dictyonema beds (divi- sion 3c) at Navy island, St John harbor, and doubtfully referred by him to the Lower Tremadoc form, Linnarssonia belti Davidson! It agrees at least with this St John fossil in size, outline and horizon. The internal characters of the latter are not well known. ) ‘ Nat. Hist. Soc. New Brunswick. Bul. 19. 1900. 4:275, pl. 5, fig. 5a-g. * Roy. Soc. Can. Proc. and Irans. 1891. 9:43. | > U.S. Nat. Mus. Proce. 1902. 25: 577. “Roy. Soc. Can. Proc. and Trans. 1891. 9:42. 912 NEW YORK STATE MUSEUM The Dictyonema bed in Scandinavia If we wish to arrive at a proper valuation of the importance of the Dictyonema horizon for the determination of the upper boundary of the Cambric, we must turn to northern Europe, where the subdivisions of the Cambric and Lower Siluric ter- ranes have been studied most extensively, and the Dictyonema Slate has long been known. A lucid discussion of the relations of the Upper Cambric to the Lower Siluric has there been fur- nished by Professor Brégger in his paper, “ Ueber die Verbrei- tung der Euloma-Niobe-Fauna (der Ceratopygenkalk fauna) in Europe.”! Frech? has also discussed the problem of the upper limitation of the Cambric in an able and concise manner. We learn from these treatises that in Sweden, and still more . in the Baltic provinces of Russia, the boundary between the Cambric and Siluric is most sharply defined; that there is a break in the deposition, and that an entire change of the faunal associations leaves little doubt as to the boundary line. In Norway, however, as Brégger has well shown in his “ Die siluri- schen Etagen 2 und 3 im Kristianiagebiet ete. 1882,” a gradual transition takes place between the beds assigned to the Cambric — in Sweden and to the Lower Siluric Ceratopyge limestone. Here the boundary, as Brégger states, has to be drawn by “ charac- - teristic peculiarities in faunistic features.” The same distin- guished author states [loc. cit. p. 79] in regard to the region of Christiania : It can not be denied, that in the beds below the Dictyograptus shale the fauna bears throughout a primordial (Cambric) char- acter; no graptolites, no cephalopods, no trilobites of the type of the characteristic Ordovicic genera (Asaphidae, Trinucleidae, Cheiruridae, etc., etc.). Immediately above the Dictyograptus shale itself we find simultaneously the first richer graptolite fauna (Bryograptus zone), the first Asaphidae (Symphy- Surus incipiens Br6ogger) and soon also the first cephalo- pods (Orthoceras atavus Broégger), in the Ceratopy- genkalk, in the region of Christiania and correspondingly also in the fauna of Hof, of the Shineton shales, etc. There seems then to remain only the possibility of placing the boundary at the Dictyograptus shale itself. I have hence united this with the Cambric. ' Nyt. Mag. for Naturvidensk. 1896. B. 35, 5S. 164-240. 2 Lethaea Palaeozoica. 1897. 2: 30-34. REPORT OF THE STATE PALEONTOLOGISY 1902 943 It is further stated, that, while to some degree the Niobe- Kuloma fauna has still a mixed character, and contains primor- dial forms (specially Olenidae), the typically developed fauna of the Ceratopyge shale and still more of the Ceratopyge limestone in Norway is in most prevailing degree a Lower Siluric fauna. Frech states that not a single species of trilobites goes beyond the Dictyonema shale into the Ceratopyge limestone in Sweden, in Norway Cyclognathus micropygus passes still into the Symphysurus bed, but not into the Ceratopyge shale; while, on the other hand, there appear not less than three new families and 13 genera above the Dictyonema bed. Therefore Broégger’s claim appears fully justified: The northern paleontologists, almost without exception, have always agreed to place the termination of the primordial fauna at the Dictyograptus slate; thus have done Linnarsson, Lind- strém, Nathorst, Tullberg, Holm, Lundgren, etc. in Sweden; that have I done similarly for Norway. If one therefore will use the term “ Cambrium” for the pri- mordial-siluric sediments . . . then in my view one must also in England, Wales, France, America, etc., if this term shall be defined reasonably, put the upper linvit of the Cambrium there where the second, to use Lapworth’s name, the Ordovicic fauna be- gins, i. e. immediately above the Dictyograptus slate. : The Cambric of the Baltic provinces of Russia has been thor- oughly investigated by Fr. Schmidt... It shows considerable modification from the typical development in southern Sweden. The black shales so characteristic in Scandinavia have thinned out, and soft and seemingly not very old deposits appear in their place. It is divided by Schmidt into three stages, (1) the Blue clay, (2) the Ungulite grit, and (3) the Dictyonema slates, which form the characteristic uppermost zone of the system. Of this it is said: This, stage (3), the Dictyonema slate, is the highest member of our Cambrian series, and a very important one too, as it is the only indubitable connecting link between our Cambrian and that of Scandinavia. The Dictyonema slate has a thickness of from 1 to 10 feet and is exactly identical with the same stage as developed in Sweden and Norway. * Geol. Soc. Quar. Jour. Nov. 1882, p. 516; Acad. Imp. Sci. St Petersburg. Mém, 2. 1889. v.36. ‘944 NEW YORK STATE MUSEUM As its characteristic species is cited Dictyonema fla- ‘belliforme KEichwald. In some places the Dictyonema ‘slate shows also some other graptolites, which Schmidt believes ‘to be identical with Bryograptus kjerulfi Lapworth. Also on the islands of Oeland (Moberg) and Bornholm (John- strup) the Dictyonema zone has been found, and in Belgium D. flabelliforme has long been known. It occurs there in the eastern part according to Malaise, and forms, as Dewalque asserts, as definite a horizon as it does in Wales and Scandinavia, in the lower part of the systéme salmien above the -systéme revinien. | The Dictyonema bed in Great Britain If we turn now to Great Britain, we find that there also the Dictyonema zone is well developed, in north and south Wales ‘and in Shropshire, and that Dictyonema flabelli- forme has long been known as Dictyonema sociale Salter. But the zone is placed here at the base of the large mass of dark gray slates, to which Sedgwick gave the name ‘Tremadoc slates, and which he inclosed in his Cambric system. ‘The bitter controversy between Murchison and Sedgwick in- ‘volved the position of this terrane, like that of the Lower Siluric ‘terranes, in much uncertainty, but it appears that the consensus of the British geologists is now to consider the Tremadoc as a part of the Cambric and thus to place the Dictyonema shale at about the base of the Upper Cambric. This is clearly and ob- jectively expressed in Geikie’s Textbook of Geology, 1892, p. 729, where we read: ; It is at the top of the Tremadoc strata that the upper limit of the Cambrian or Primordial formations is now drawn in Britain . . . There appears to be more satisfactory proof of a distinct paleontological break at this stage of the geological record in Britain, or at least between the lower and upper part of the Tremadoc subgroup. This proceeding, which, as an incidental result, separates the Dictyonema slate from the accepted base line of the Lower Siluric by 1000 feet of strata, is at variance with the views of the continental geologists, as is shown clearest by the publica- tions of Professor Brégger and the new edition of the Lethaea Palaeozoica. It finds its explanation, besides the historic reasons, REPORT OF THE STATE PALEONTOLOGIST 1902 945 in the fact that the relations of the Tremadoc to the Cambrie, on account of the frequency of the Olenidae and Lingulellae in the former, are more striking than those of the Ceratopyge beds to the Olenus shales in Scandinavia. | Professor Brégger’s careful revisions of the determinations of the English paleontologists [see his two works cited before] leave however little doubt, that, as Brégger concludes, the Tremadoc is to be correlated with the Ceratopyge beds, and hence the Dictyonema shale is to be regarded also in Britain as the terminal member of the Cambric series. The Dictyonema beds of the Malvern hills overlie the “ Dolgelly group” and are placed by Callaway! below the “ Shineton shales”. The latter are considered by the same author as transitional between the - Lingula flags and the lower Tremadoc, and thus still placed with the Cambric. Brégger, however, subjects the genera of the “Shineton shales” to a revision? and thus finds the latter to be equivalent to a horizon between the Dictyonema bed of Norway and the Ceratopyge limestone, approximately to his 3 aa—d @%; thus transferring them into the Lower Siluric. The Tremadoc of north Wales has been worked out by Salter.* Brégger concludes as to the Tremadoc of North Wales (in “ Ueber die Verbreitung etc.” p.42) that its largest part is equivalent to the Ceratopyge limestone horizons 3 aa—s aY, that the lowest part of the Tremadoc (with Dictyonema flabel- liforme) corresponds already to his zone 2 e, the Dictyo- graptus slate of Christiania, while the uppermost part is per- haps equivalent to his 3 b, the Tetragraptus-Phyllograptus slate of Christiania. The Tremadoc beds of south Wales (St Davids and Ramsay island) have become known, specially by the investigations of H. Hicks. They differ considerably from the development in north Wales and in Norway, consisting of more than 1000 feet of gray, flaggy sandstones (St Davids) with few trilobites and 1 On a New Area of Upper Cambrian Rocks in South Shropshire with a Description of a New Fauna, Geol. Soc. Quar. Jour. 1877, 33: 652 ff. ? Etages 2 and 3, p. 144-46. * Mem.‘of the Geol. Sur. 1866. v.3. See edition of 1881 by Etheridge. See also A Monograph of British Trilobites (1864-83) in Pal. Soc. and,Cat. of Camb. and Silur. Fossils. 1873. * Geol. Soc. Quar. Jour 1873. 29:39 ff. 946 NEW YORK STATE MUSEUM a relatively rich lamellibranch fauna. In regard to these, Brégger disagrees with Hicks’s view of considering their fauna as closely allied to the Lingula flags, but holds that the species of — Neseuretus and the lamellibranch fauna point to a younger age. and indicate a shallow water facies of the deeper water deposits of the Tremadoc of north Wales, with which he correlates these beds. The latter would, then, also have to be transferred to _ the Lower Siluric. They are also underlain by the Dictyonema slates; which accordingly would also in Wales denote the upper boundary of the Cambric, instead of falling within the Cambric as held by Salter, Callaway and Hicks. | | Frech shares the views of the Seandinavian geologists as to the parallelization of the Scandinavian and British Cambrian- Silurian beds and holds with Brégger, that, though the relations of the English Tremadoc to the Cambric are more distinct than those of the Ceratopyge limestone to the Cambric on account of the prevalence of the Olenidae and Lingulellae, this fact is not of conclusive importance, as the Tremadoc is characterized, like the Ceratopyge limestone, by the appearance of those tri- lobite families which reach their principal development in the Lower Siluric. The Asaphidae, Lichadae and Ampycidae appear immediately above the Dictyonema slate; the Cheiruridae and Trinucleidae occur already in numerous representatives in the Upper Tremadoc; while the Olenidae and Conocephalidae of the Cambric are represented only by genera, not pertaining to the Cambric proper, as Ceratopyge, Euloma, Remopleurides, etc. Frech concludes that no doubt can be entertained as to the Lower Siluric position of the Tremadoc terrane and adds that the confusion existing in England in regard to the boundary of Oambric and Siluric excludes a solution of the problem by recog- nizing the rights of historic priority. Professor Kayser also, in his Geol. Formationskunde, which has just appeared in a new edition (1902, p.48), holds that the Dictyonema bed forms the top of the Lingula shale and not the base of the Tremadoc shale, as the English geologists maintain, and further that the Tremadoc is a part of the Siluric formation ; that hence, also in England, the Dictyograptus bed closes the Cambric formation. | REPORT OF THE STATE PALEONTOLOGIST 1902 947 In combining all the facts, viz that the underlying Dolgelly beds contain well known European and also eastern American Upper Cambric horizon markers, such as Peltura scara- baeoides, and the overlying Tremadoc terrane as distinctly Lower Siluric forms such as Calymmene blumen- bachii, while the graptolites, on account of their pelagic life, have a wide horizontal and very limited vertical distribution and are themselves extremely exact indicators of synchrony, we be- lieve it does not infringe on the rights of British geologists to conclude that the Dictyonema flabelliforme zone is in Britain as in the rest of Europe to be held as marking the ‘ top of the Cambric series, wherever it is observed. The Dictyonema bed in North America The first to publish a notice on the occurrence of the Dictyo- nema bed in America was, so far as we know, Sir William Dawson! Sir William reports that Mr Richardson found at Matane “a bed of highly laminated black shale similar to that explored by Mr Weston a few years ago at Little White river, holding similar fossils in great abundance. Prominent among them is a beautiful Dictyonema, distinct from any of these found at Levis, and which on comparison with specimens presented to the museum by Prof. H. Alleyne Nicholson, appears so close in all its characters to D. sociale Salter, of the Eng- lish Tremadoc, that it may fairly be assumed to represent that species in our fauna. It is well known that some good paleon- tologists regard D. sociale as only varietally distinct from D. flabelliforme of Eichwald from Russia. . . We might infer from this that the Dictyonema beds at Matane may indicate a horizon somewhat lower than any of those at Levis. Associated with the Dictyonema are many specimens of Dichograptus (corrected in handwriting for Didymograp- tus) flexilis and D. logani, or an allied form, and there are also fragments of an undetermined Tetragraptus.’” —$—$—— * Peter Redpath Mus. of MacGill Univ. 2d Rep. Jan. 1883. p. 16. * We have no doubt that the species of Dichograptus cited here refer to the Cambric species of Clonograptus, either toCl. proximatus Matthew or Cl. milesi Hall, specially as also elsewhere these Cambric Clonograpti have been first compared with the Beekmantown Clono graptus Dichograptus) flexilis. 948 | NEW YORK STATE MUSEUM It is added that in a neighboring bed there is a vast quantity of debris of trilobites, which seem to agree with the graptolites in indicating an Upper Cambric age, as they are apparently more nearly related to the trilobitic fauna of the Potsdam of Newfoundland, as described by Billings, than to that of Levis. Sir William Dawson’s conclusion of the presence of an Upper Cambric graptolite zone at the lower St Lawrence river has a few years later been verified by Prof. Charles Lapworth from material which had been submitted to him by the Cana- dian Survey. In his report! Lapworth recognizes three zones namely, in descending order, the Griffin point or Marsouin rwer zone (zone of Coenograptus gracilis) which corre- sponds to the Normans kill beds of New York, the Ste Anne zone (zone of Phyllograptus anna) which has been recognized in the middle of the three Deep kill graptolite zones, reported on in a former paper, and finally the Cape Rosier zone (zone of Dictyonema sociale and Bryograptus). It is tbe last zone which this year has been found fully rep- resented within the slate belt of eastern New York. We quote those remarks of Lapworth’s on this zone, which seem important to our inquiry. 3 The oldest graptolitic zone represented is the Dictyo- nema sociale zone of Barrasois river (Cape Breton island) and of Cape Rosier, Gaspé. There are very few specific forms occurring in this zone, but they constitute together a very peculiar and distinct group, totally different from those of the remaining zones. The genera include Dictyonema, Bryograptus and Clonograptus, together with the dubious genus Staurograptus of Emmons. The Dictyonema appears to me to be absolutely identical with one of the forms referred by European (Scandinavian) geologists to Dictyonema_ flabel- liforme KEichwald, which is also, so far as our present eyvi- dence enables us to judge, identical with Dictyonema sociale Salter, from the Tremadoc of north Wales. To this zone belong the Barrasois river beds, those of Cape Rosier, of Little White river, of Grand Méchin point, of half a mile west of Long point, Matane, Little Capucin river, etc. Preliminary Report on some Graptolites from the Lower Palaeozoic Rocks. on the South side of the St Lawrence from Cape Rosier to Tartigo River, from, the North shore of the Island of Orleans, etc. Roy. Soc. Can. Proce. and Trans, 1887. 4:167-84, REPORT OF THE STATE PALEONTOLOGIST 1902 - 949 In Europe, this zore (or zones) occurs in the Tremadoc of ‘Wales and the Tremadoe and Ceratopyge beds of Norway ‘(Brégger) and Sweden (Tullberg). It is Upper Cambrian (as British geologists receive the term), and is probably represeiited in the West by a part of the Calciferous series of New York and ‘western Canada. It is distinctly older than the graptolitic mass of the Point Levis beds. Nut one of its forms has hitherto been figured from the Quebee group. if may occur at Point Levis, if the Calciferous is represented there. This is a point for future ‘discovery to settle. In the meantime, however, it will be better to refer to the zone as the “ Cape Rosier zone.” Like the Levis ‘Calciferous conglomerate beds, its fauna is made up of genera, partly Cambrian and partly Ordovician (i. e. partly Primordial and partly Cambro-Silurian). The Cambrian age of the Dictyonema- bearing Barrasvis river beds of Cape Breton island is demonstrated by their included ‘Olenidae. The Dictyonema beds of Gaspé and Méchin can not be far above this Cape Breton zone. It is exceedingly probable, therefore, that, as in Cape Breton, the Dictyonema beds lie not far removed ean the unconformable base of the fossil-bearing ‘rocks of the district. From further statements of the same author it can be con- ‘cluded that he was averse to paralleling definitely the Cape ‘Rozier zone with any formation of the New York series; for instance, in the summing up on page 174, we find under Cam- bric formations: B! Fine conglomerates . . . and black slates (of Shick- ‘shock range). B? Gray, red, brown and black shales with beds and bands ‘of dolomite (Localities: Les Islets, coast south of Cape Rosier, ‘etc). Fossils: Dictyonema, Bryograptus, etc. To this is added (B! and B? may, perhaps, represent both the Upper Potsdam ‘and the Calciferous rocks of the western district of New York ‘and central and upper Canada.) | In the table on page 183, the zone has been divided into two ‘subzones, as follows: B Dictyonema sociale zone (A). Shales of Cape Rosier, Little Whale river, Grand Méchin point, with Bryo- ‘gra Pp tus Ssp., Stauvorraptus, ee eve, Dictyonema ‘sociale Salt. Dictyonema zone (B). Shales of Barrasois river, eaaecBraiin end, yah » bet a2 onema soc 1 a : € ey rae Plenidae. fon have aie on led 6 the discovery of the Diety onema zone 950 NEW YORK STATE MUSEUM in the beds of the St John basin in New Brunswick.t Mr Mat- thew had, in full appreciation of the importance of D. fla- belliforme for the determination of the upper boundary of the Cambric system, searched for years for this fossil in the black shales of division 3 (Bretonian) till the desired a was found on Navy island in St John harbor. We learn from his important publications the interesting fact that in the St John basin, Dictyonema flabelli- forme is not restricted to a single zone above the trilobite zone characterized by Peltura scarabaeoides, but that this Upper Olenus fauna extends in the Canadian Cambric into the Dictyonema zone, since its trilobites occur in lentils with layers included in shales which contain the Dictyonema. Mat- thew’s practice has been to “ regard the beds above the horizon to which these trilobites, so far as known, are limited, to be the true zone of Dictyonema, corresponding to the beds so desig- nated in Europe, and to include the beds below, in which Lepto- plastus, Sphaerophthalmus and Peltura are found, and which also contain Dictyonema, as a lower zone corresponding to the upper part of the Upper Olenus zone as developed in Wales and Scandinavia.” He obtains thus the following zones of the Bretonian division of his St John group: a Zone of Parabolina spinulosa . b Zone of Peltura scarabaeoides, contains also Dictyonemea. tlabellitorace . e Zone of Dictyonrema’ flabellitor me). tpred development of the species This is followed by an interruption of sey Sil hundred feet, the fauna of which is not known, and then by the Lower Siluric Phyllograptus shales. — | These results obtained in the St John basin are important in several regards: they prove that Dictyonema flabelli- forme is not everywhere restricted to a single graptolite hori- zon, but may range through a considerable thickness, and that its beginning falls distinctly into the hemera of the last trilobites * See On a New Horizon in the St John Group, in Canadian Record of Science, October 1891, p. 389-43, and Two New Cambrian Graptolites with Notes on other Species of Graptolitidae of that Age, in N. Y. Acad. Sci. Trans. Aug. 1895. p. 262-73, pl. 48 and 49. REPORT OF THE STATE PALEONTOLOGIST 1902 951 of the Upper Cambric, as was clearly indicated by Lapworth’s investigations. There can hence be no doubt that even where the Dictyonema zone contains no characteristic fossils of the Upper Cambric beds, it should be united with the latter and not with the succeeding graptolite faunas of the Lower Siluric. Lately! Dr Matthew has also described the Dictyonema zone as overlying the Peltura zone from Cape Breton island. Dr Ells’s exhaustive Report on the Geology of a portion of the Province of Quebec? and the appended list of fossils by Dr Ami? prove that in the classicai region of Logan’s Quebec group the Dictyonema bed has not yet been observed. In citing Lap- worth’s correlation of the Dictyonema zone, and remarks (p. 48k) Dictyonema sociale zone is mentioned as “ presum- ably Cambrian,” and it is added ‘that Dictyonema has not, in so far as is yet known, been figured from the Point Lévis beds, the most westerly point from which it is reported being Matane.” | Dr Ells is however inclined to doubt the correctness of Lap- worth’s correlation of the Dictyonema zone, and remarks (p. 48k) that Lapworth considers the Dictyonema zone from the presence of three species to belong to a lower formation than the Cambro- Siluric, and that of these two, a Clonograptus and a Dicho- graptus are apparently new and therefore not conclusive. The presence of Dictyonema appears, then, to be the only reason why those portions in which this form is known to occur, otherwise intimately associated with strata holding Cambre- Silurian fossils, and which have so long been regarded as be- longing to that group, should be removed from their apparently proper position in the series and placed in a different geological System; and, in view of the wide range Dictyonema is known to possess, we may well hesitate before deciding on such a separa- tion, unless confirmatory stratigraphical evidence can be pre- sented. While this conservatism at the time of the publication of the report was justified to some extent, the facts brought out by _ Matthews’s and Broégger’s investigations serve to dispel all ‘Roy. Soc. Can. Proc. and Trans. 1891. p. 360, Nat. Hist. Soc. New Bruns- wieeul 19. 1900. 4:219; zbid. no: 20. 1902. v. 4, pt 5, p. 377 ff. *Geol. and Nat. Hist. Sur. of Canada. ser.2. 1888. vy. 3, pt 2, p. 5k-114k. Ibid. p. 116k-120k. ‘Ibid. p. 45k. 952 ee NEW YORK STATE MUSEUM doubts about the reliability of Dictyonema flabelli- forme as an Upper Cambric index fossil. Dr Ells determines the stratigraphic succession of the fossili- ferous Quebec terrane(p.63k-64k; Cape Rouge section) as follows: 1 Black, green and gray shales, with thick bands of quartzose sandstone and occasional thin bands of limestone conglomerate. (Lower Sillery) 2 Mostly greenish, grayish and blackish shales with thin lay- ers of gray sandstone. On the south shore of the St Lawrence, below Levis and also on the south shore of the island of Orleans, beds of conglomerate occur at about this horizon, in which the Lower Cambrian fauna occurs (Olenellus thompsoni). 3 Bright red shales, with thin bands of greenish and gray shale. the upper part, near Sillery, and on the south side of the river Obolella pretiosa, Protospongia fenestrata, Phyllograptus typus, Tetragraptus serra and Lingula quebecensis. 5 Levis shales and conglomerates of Point Lowe (Cale = @ erous). 6 Black and grayish striped or banded shales, etc. (Upper Chazy or Lower Trenton). , | 7 The black or brownish bituminous shales and limestones of the city of Quebec and northwest side of the island of Orleans. The contained fauna is of Trenton-Utica age. In regard to a correlation of the Cape Rosier or Dictyonema zone of the Lower St Lawrence shore, we find in Dr Ells’s report (p. 82k) the following statement: From Métis to Cape Rosier the great bulk of the rocks belongs to the Sillery formation and much of it to the lower portion of that division, and entirely below what we regard as the fossiliferous or graptolitic Lévis formation of the city of _ Lévis and the southwest end of the island of Orleans. . The rocks of Cape Rosier, in which the Dictyonema Sociale, Clonograptus, etc., were found, as well as those 2 miles below Great Matane river, where similar forms occur, represent divisions 2 and 3 of the Cape Rouge section and the - Beaumont shore, as well as of the strata on the south side of the island of Orleans, consisting of black, green and gray Shales, with some red beds, together with the gray limestones and hard, grayish quartzites, while the associated limestone — conglomerates are like those seen at Beaumont and at the east 4 Red, seniaial eray and black shales, with interstratified sandstones (Upper Sillery). Obolella pretiosa occurs in REPORT OF THE STATE PALEONTOLOGIST 1902 953 end of the Island of Orleans. This character is maintained with great uniformity for the entire distance west of Marsouin, though at certain points the Sillery sandstones and red and green shales representing division 4 are more highly developed than at others. The rocks of this section would, therefore, both on the evidence of Professor Lapworth from the fossils, and from the comparison with the stratigraphical sequence of the Cape Rouge rocks, belong to a portion of the Cambrian system, probably representing the upper and middle divisions of that system, while the overlying Levis graptolitic shales and lime- stone conglomerates would represent the lower portion of the Ordovician or Cambro-Silurian system. Dr Els refers thus, on the evidence afforded by the strati- graphy and the graptolites, determined by Lapworth, the Sillery rocks (divisions 1, 2, 3 and 4) to the Cambric, and the Levis beds (division 5) to the lower Beekmantown. | Mr Walcott, in his review of Dr R. W. Ells’s report? takes exception to some of Dr Ells’s conclusions, as we see from his quoted statements: The Cape Rosier Dictyonema sociale zone is regarded as the lowest of the graptolitic zones, and to indicate the horizon of the Tremadoc terrane of Great Britain. The Cape Rosier beds are referred to the Upper Cambrian by Professor Lapworth and Dr Ells, but, with our present knowledge of the Cambrian in America, I would refer them to the Lower Ordovician or to the lower Calciferous. The occurrence of the typical Calciferous fauna within one hundred (100) feet of the base of the Levis series, at St Joseph de Levis, points very strongly to considering the graptolitic fauna of the Upper Sillery to be of Calciferous age, if a comparison is made with the Phillipsburgh section. Dr Ells refers the Sillery series to the Cambric, and in this I mainly agree with him, except that the upper portion is evi- dently a passage series between the Cambric and Lower Silurie. On lithologic and stratigraphic evidence the line would be drawn at the summit of the red shales. On paleontologic evi- dence, as furnished by the graptolites, I would include the upper portion of the Sillery red and green beds in the Lower Siluric, as I think they are above the typical Potsdam zone of America. While we agree with this distinguished author in referring the upper part of division 4, containing Phyllograptus *Am., Jour. Sci. ser. 3. 1890. 39:113. 954 NEW YORK STATE MUSEUM typus and Tetragraptus serra, to the Beekmantown, the Cape Rosier Dictyonema sociale zone should, in our opinion, on the evidence adduced above from northeru Europe and specially in view of the fact that in the St John basin it is found in the same beds with Cambric trilobites, be retained in the Cambric system. Dr Ells correlated this zone with divisions 2 and 3; as division 2 however contains Lower Cambric fossils, the Dictyonema zone should be expected at a much higher level, and we surmise that, if it is ever found in the Quebec region or Cape Rouge section, it will appear in the lower or middle part of division 4, or just below the line, where Walcott would terminate the Cambric system. | | We have already stated in the report on the Levis beds of the: slate belt that Professor Dale! recognized the presence of a terrane (horizon F) of ca, 35 feet of “ gray, calcareous or very quartzose, finely bedded shales or black shales, with thin lime- stone beds”, which he referred to the Beekmantown. Dr Gurley identified in the suite of fossils submitted to him for this ter- rane, Bryograptus, Dichograptus, Callograptus salteri? ef. Dendrograptus sp. and Dictyonema flabelli- forme. In regard to this fauma it is said: ‘ Several of these are regarded as probably of Calciferous age, which would place the horizon in the lowest part of the Ordovician. The European species of Bryograptus come from the Upper Cambrian. Dictyonema ranges from the Ordovician into the Devonian.” The cited list of determinations gives us the impression that Gurley had before him fragmentary representatives of both the Cambric Dictyonema and Lower Siluric Phyllograptus zones. There is no doubt that, with his thorough knowledge of the graptolites, Dr Gurley would not have failed to recognize the zones mentioned, if such complete collections as the writer has, had been at his disposal. But any one who is at all acquainted with the slate region of Vermont and eastern New York, knows the extreme difficulty of securing anything but fragmentary col- lections in the intricately folded and mostly strongly cleaved beds. Exceptionally fortunate circumstances are necessary to permit the collection of superior material. } U.S. Geol. Sur. 19th An. Rep’t 1899. p. 185. REPORT OF THE STATE PALEONTOLOGIST 1902 955 The fact, that the Upper Cambric Dictyonema and the Lower Siluric Phyllograptus zones have apparently been united by Dale in his horizon F, demonstrates the lithologic identity of the beds, also observed by the writer and suggests, as stated before, the continuation of the same physical conditions from the Upper Cambric into the Lower Siluric time. Possible subzones of the Dictyonema horizon Whether the Dictyonema bed of New York will ever admit a further division into subzones, we are at present unable to sur- mise. In Norway Brégger has found that the mut. norvegica lies a little higher than the typical Dictyonema flabellti- forme. In Sweden, Linnarsson, in 1871, had already discerned a zone with Clonograptus tenellus Linn., which was at first thought to lie below the Dictyonema flabelliforme zone, and to be associated with the Cam- bric trilobite Sphaerophthalmus alatus. Moberg! has, however, shown that this form lies above Dictyonema flabelliforme, and that the latter species occurs. in layers immediately adjoining those with Sphaerophthal- mus alatus. | Not very long ago Anton Nilsson and Axel Tellander? demon- strated that also in southern Sweden (near Fogelsang, Lund. Sheet) several zones can be discerned, namely, in descending order : Zone with Dictyograptus norvegicus Kjerulf and Bryograptus kjerulfi Lapw. Zone with Clonograptus ef. flexilis Hall. Zone with Dictyograptus flabelliformis Eichw. forma typica. Their observations verify Broégger’s statement of the occur- eeemee OF Dictyonema flabelliforme var. norve- Secum and of Bryograptus kjerulfi ‘above the typical Dictyonema flabelliforme. Matthew’s results did not suggest to him a possible separa- tion into a Clonograptus and Dictyonema zone. At Schaghti- coke the two occur separated, but it is impossible to say posi- sce TIS SS SZ 55 UU 2c kA ‘Sver. Geol. Unders. Afhandl. och upps. ser. C. no. 125. 1892. p. 1-16 * Geol. Féren. Férhandl. no. 201. 1900. 22:421-26. 956 NEW YORK STATE MUSEUM tively which lies higher. The occurrence of still another Clono- graptus, Cl. milesi Hall, in black shales near Georgia Vt., indicates however that there may be Cambric subzones, charac- terized by forms of Dictyonema and the two species of Clono- graptus. These subzones may lead very gradually into the Tetragraptus and Phyllograptus zones of Beekmantown age; for the occur- rence of a Clonograptus ef. flexilis Hall (a Point Levis form) between the two Dictyonema horizons reported by Nilsson and Tellander and the finding of a typical specimen of Bryograptus kjerulfi in the Tetragraptus shale of the Deep kill by the writer, as well as some other facts of dis- tribution, would indicate the presence of such transitional zones. between the Dictyonema and Tetragraptus beds. These would be equivalent to the Ceratopyge beds of Scandinavia, which there intervene between these graptolite beds, and to the Tre- madoc of Britain. , Bearing of the occurrence of the Dictyonema bed on Cambric paleogeography Messrs Ulrich and Schuchert have undertaken the task of elaborating a theory in explanation of the differences in stratigraphic succession and faunistic aspect of the Appala- chian region and the area to the west of the same during paleo- zoic time’. The solution is found in the assumption of the pres- ence of one, or at times, two parallel basins, separated by and inclosed in folds or barriers, and extending during the greater part of the Paleozoic over the territory of the present system of Appalachian folds. This theory not only serves to clarify a multitude of well known stratigraphic and paleontologic facts, but is also an incentive to investigations in fcrther elaboration or modification of its details. The facts presented in this paper furnish, on one hand, a new argument for the presence of such basin, and, on the -other, appear to necessitate a modification in regard to the fixation of the date at which one of them, the Levis basin, is supposed to have originated. 1 Paleozoic Seas and Barriers in Eastern North America. N. Y. State Paleon- tologist. An. Rep’t. 1901. p. 633-63. Oo REPORT OF THE STATE PALEONTOLOGISYT 1902 957 We have seen that the Dictyonema fauna is an undoubted Atlantic fauna. In North America it has been recognized in the St John basin of New Brunswick, on Cape Breton island and at several places on the south shore of the St Lawrence from Cape Rosier to Matane river. It has now been found as far south as Rensselaer county in New York and probably ex- tends through the slate belt of New York and Vermont. It is hence, with the exception of the Levis region, where it has not yet been found, about coextensive with the present known ter- ritory of the Phyllograptus fauna. Like the latter, it has not been found either east or west of this long be!t and is therefore to be assumed to have entered from the Atlantic, a basin of Similar configuration and extension as the Levis channel, in which the Atlantic waters deposited the Phyllograptus fauna. The Dictyonema shale is now however of Upper Cambric age, of which it represents the closing period wherever it has been found. It stands, lithologically and faunistically, in the same relation to the upper Potsdam of the Champlain region as the later Phyllograptus shales to either the Beekmantown beds, with which the writer correlated them, or to the Chazy beds, with which they are equivalent according to Ulrich and Schuchert’s views. The Dictyonema beds represent, like the Phyllograptus Shale, the graptolite shale facies of a trilobite-gastropod-bearing limestone (or sandstone in part) which adjoins the slate belt closely to the west and northwest. Ulrich and Schuchert see in the parallelism of the two different faunas and rock series (Phyllograptus shales and Chazy limestone) proof of the pres- ence of twin channels, the Levis channel and Chazy basin, stat- ing that “the respective faunas and the lithologic character of the deposits in the twin channels are so different that we can not doubt the thorough effectiveness of the Quebec barrier dur- ing the whole of Chazy time.” Accepting, for the purpose of further argument, the correctness of the postulation of this bar- rier to explain the stated facts, it follows that a like barrier of equal extent must be postulated for the late Cambric time, and that the beginning of the elevation of this “ Quebec” barrier, the northern extension of the “Appalachian valley fold”, must be placed in late Cambric time, instead of at the beginning of 958 - NEW YORK STATE MUSEUM Chazy time. Toward the east the Levis channel was bounded by the Green mountains fold, which is supposed to have already emerged in middle Cambric time. This, as far as our knowledge goes, bounds also the upper Cambric graptolite shale. Ulrich and Schuchert hold that the region of the later Levis channel had emerged during the Potsdam period, [see the un- classified time scale, opposite page 658, J. c.].. This is in accord- ance with Professor Dale’s conclusions,! who not only found the middle and upper Cambric beds to be missing, but also observed an unconformity between the Lower Siluric and Lower Cambric, indicating the emergence of the lower Cambric beds during the succeeding Cambric time. Our observations agree thus far fully with these results of Mr Dale’s elaborate investi- gation with the exception of the closing upper Cambric time, represented by the Dictyonema shale. Toward the west and north of this strip of upper Cambrice land, forming the “ Vorland” of the Green mountain fold,. ex- tended the more or less broad ‘St Lawrence channel,” which effected the communication between the Atlantic and Missis- Sipplan seas, indicated by the distribution of the Dicellocephalus fauna. The question whether this late Cambric “ Levis ” channel per- sisted throughout the Beekmantown period in this southern part of the present slate belt or the broader St Lawrence channel extended freely from the Adirondacks to the Green mountains is a problem, the solution of which is dependent partly on the exact correlation of the limestones occurring in the slate belt and partly on that of the three Deep kill zones of graptolites, corresponding to the Phyllograptus horizons of Europe. It will necessitate much detailed investigation to obtain conclusive facts and to decide between the differing views held in regard to these beds. | * New York-Vermont State Belt, U.S. Geol. Sur. 19th An. Rep’t. 1897-8. ON THE SEDENTARY IMPRESSION OF THE ANIMAL WHOSE TRAIL IS KNOWN AS CLIMACTICHNITES BY JAY B. WOODWORTH In the course of an examination of the Pleistocene deposits of the Mooers quadrangle, including the township of Mooers, in Clinton county, N. Y., in the summer of 1902, I had my atten- tion called to certain trails on the Potsdam sandstone in that town which are remarkable for their distinctness and association with terminal impressions not heretofore described. Having seen the trails of Climactichnites on a flagstone in the main street of the village of Mooers, I was led to inquire for the quarry whence the stone was derived, and, though I did not learn whence the slab came, I was informed by the postmaster of the tracks which it is the object of this paper to describe. The trails (Climactichnites) described in this paper occur in the town of Mooers on the west side of the Mooers branch of the Delaware and Hudson Railroad a few rods south of what is known locally as Bidwell’s crossing, on the land of Mr B. H. Palmer, at the first rock cut in the railroad north of Sciota and distant from that station somewhat less than 2 miles: The Potsdam sandstone is here practically horizontal and is exposed in the rock cut as a badly shaken, irregularly splitting series of prevailingly light colored sandstones. The track layer is exposed in the adjoining field in the wave-swept trough between two of the small beach ridges of the postglacial marine stage of the Champlain valley. The track layer, where its edge is exposed, has a thickness of 8 inches; it is traversed by several rudely parallel joints cutting all of the longer trails. The area ex- posed at the time of my visit was about 50 feet long and varying in width from a yard to over two yards. The trails appear to have been first noted by the present owner of the land, who states that he cleared away some of the surface debris several years ago. Locally the trails are spoken of as those “serpents,” and the impressions associated with them as “human footprints.” A visit to the locality confirmed the surmise that the “serpent trails” are the ladderlike tracks known as Climactichnites. What, so far as I know how- 960 NEW YORK STATE MUSEUM ever, is new is the occurrence at this locality of impressions at, the end of the ladderlike trails, giving rise to the so called, “ footprints.” The trails called Climactichnites, first made known by Sir. William E. Logan from Beauharnais, Canada, have since been found in Wisconsin and at Port Henry, in this State. In the 42d annual report of the State Museum for the year. 1888, an account with illustrations is given of the trails from, certain of these localities, including the original description of Climactichnites wilsoni. For other references to, the literature, the reader should consult Professor Hall’s! report. Opinion as to the origin of climactichnite trails has been ex- tremely varied. From their occurrence in strata in which large. trilobites are the only known animal remains with which the trails can be associated, there has been a prevailing belief, ex- pressed by Sir William Dawson, Dana, and others, that the. tracks are probably those of a crustacean if not a trilobite. Nicholson? has .expressed the view that Climactichnites was, probably formed by the same animal which produced Protich- nites, and notes that Sir William Dawson observed that the living Limulus or horseshoe crab, when it uses its swimming. feet, gives rise to a ladderlike trail. Sir William Dawson, in, his comparison with the trails made by Limulus in different: modes of progression, notes that in the case referred to, where. the platelike swimming organs pile up transverse ridges of sand, the lateral_and medial lines which are produced at the same. time are furrows and not ridges as in Climactichnites. T. Rupert: Jones! was inclined to compare the trails with the galleries of burrowing crustacea. Professor Chapman® believed that both, Protichnites and Climactichnites are really of vegetable origin... Still others, including Logan, have regarded the trails as having. been made by a gastropod or an annelid. ‘Hall, James. N. Y. State Mus. Report of the Director. 1888. p. 25-34, plate. opposite p. 34. ® Nicholson, A. Manual of Paleontology. ed. 2. 1879. 1:361. * Dawson, Sir J. W. On the Footprints of Limulus, ete, Can, Nat. 7:271-77- * Cited by Sir J. W. Dawson, p. 277. eae ® Cited by Nicholson, p. 361. a a eee V 2%Td REPORT OF THE STATE PALEONTOLOGIST 1902 961 The accompanying photographs, plates A and B, show the eastern end of the track area at Bidswell’s crossing as photo- graphed by Mr P. P. Sharples, in October 1902. Plate A is a view looking southward across the better defined trails. The point of the hunting knife rests at the end of one of the terminal impressions into which the trails merge. Other similar oval impressions are shown to the right and left. Plate B is another view of the same surface looking southeast along the two dis- tinct trails seen in the right hand side of plate A. The trails from Mooers agree in all essential characters with the original description of Climactichnites. It is to be noted that there are no traces of footprints and no medial furrow which may be attributed to the dragging of a tail spine in any portion of the trails which have been there studied. The size of the trails is quite uniform in breadth. Measure- ments show them to vary between 5 and 614 inches. The trans- verse ridges which give rise to the ladder structure are spaced _ about 1 inch apart, measured from crest to crest. Each of these transverse ridges passes on the margins into the outside lateral ridges. Regarding, for reasons shown beyond, the terminal oval impression as in the direc- tion toward which the animal was crawling in making the trail, it may be stated that the transverse ridges curve sharply forward at their margins to form the lateral ridges. This is quite evident in some por- tions of the trails, though it is not everywhere ob- vious. In figure 1, this feature is diagrammatically shown, together with the apparent overlapping of the successive ridges at their margins. The median ridge, in passing over which the transverse ridges bend rather sharply forward, as seen in the photo- graphs and in figure 1, is a sinuous line not uniformly equidistant from the margins. Another important 2%, 1. characteristic of the Mooers trails is the distinct seeenuaty pressing down of the sands in the making of the trail. °° _ By whatever process the transverse ridges were made, they were passed over and pressed on in the making. The above cited observations warrant, it appears to me, cer- tain conclusions. 962 NEW YORK STATE MUSEUM 1 The transverse ridges and their lateral extensions running forward to the next transverse ridge were made by the same movement of some organic structure lying transverse to the longitudinal axis of the organism. ; 2 The unity, identity and spacing of successive transverse ridges indicate that they were made singly and in succession, that their spacing indicates the forward stride of the organism, and that it went forward by a crawling, hitching movement. 3 The varying position of the median ridge with reference to the lateral ridges points to the conclusion that the transverse body was at the time characterized by a mesial sinus or upfold, and that the axis of this fold played to the right and left as a fold might in the flexible muscular foot of a crawling mollusk. In other words, the transverse ridges could not have been pro- duced by the successive ambulatory movements of rigid swim- ming or gill plates, or by the scraping and pressing of the sand through the application to the bottom of the posterior margin of the pygidium of a large trilobite, unless in the latter case it be admitted that the animal was molting and had not grown | a new rigid chitinous coat. 4 The pressed sand on the slopes and over the crest of the transverse ridges eliminates from the processes by which the ridges may have been made the backward push of the posterior margin of Such an animal as the trilobite or of any transverse gill plate so placed as not to permit, under the condition in which the creature moved, the smoothing down of the successive ridges by some soft, pliable body still further aw derriére. | An experiment was tried with a thin piece of board cut, as shown in figure 2, to represent the posterior margin of a trilo- bite or the inferior mar- gin of some transverse Swimming plate such as the paired gill plates Fic. 2. Side (a) and end (b) views of wooden block Which occur in the ab-— ir j duce ladderlike trails. E é used in experiment to produc arainiall region of re limuloids, with the above restrictions in mind. In order to obtain the medial ridge, it was found necessary to cut the cen- tral sinus shown in figure 2. In this way, by moving the plate dq eld REPORT OF THE STATE PALEONTOLOGIST 1902 963 in the manner indicated in figure 3, in imitation of the alternate contractile and extensile movements of a crawling organisin, whose posterior margin the plate represented, it was possible to produce transverse ridges with the medial swell and the forward curved lateral ridges apparently overlain in succes- sion by each new ridge. The whole surface of each ridge, ex- cept on the outer parts of the lateral ridges, was pressed down on both slopes, the posterior slope being steeper than the an- terior slope in this process, just as is the case with Climactich- nites. This difference of slope must necessarily arise where a transverse body is drawn for- ward, pushing up a ridge over which it is drawn in the making of the next ridge at its proper interval. “OS pushed ridge Overridden ridge. Fic. 3 Showing successive positions of scraper in experiment to imitate Climac- tichnite trails. (1) Position of scraper at end of long forward sl pe of a trans- verse ridge; (2) position of scraper after it has been raised up, overridden a trans- verse ridge, and begun to make a second frontal slope; (3) position as at 1, but showing cross section of completed trans- verse ridge in the rear. Movement ‘in direction of the arrow. Fhe experiment with the artificial plate showed that, with such a rigid body, rigid ridges only could be produced; further- more the ridges are at right angles to the margins, the central swell is equidistant from those margins, and, while the forward bend of the transverse ridge in passing over the central swell is slightly shown, the ridges themselves have not that oblique position which is frequently the characteristic feature of seg- ments of Climactichnites. The comparison of the trails natural and artificial has therefore led me to the conclusion that Climac- tichnites could not have been made by the rigid carapace of a trilobite; moreover, there is no trilobite known in the Cambrian with an outline of the pygidium which could have produced the result, nor have recent discoveries concerning the natatory organs of the trilobites shown in the group the existence of natatory or gill plates such as are found in the more modern Xiphosura. The trail itself, therefore, it seems safe to state, was made by some fiexible body like the mesially up curved 964 NEW YORK STATE MUSEUM posterior margin of the expanded, retractile foot of a large crawling organism. Jt remains to note the nature of the terminal impressions associated with many of the trails in the Mooers occurrence. In the first place, the postulate above made that the trails were made progressively toward these oval terminal impressions may now be explained by stating that, where the relation of the oval impressions to the trail can be made out, it is clear that the oval impression has obliterated a portion of the trail which once extended into the area of the oval impression; this is taken to mean that the animal which made the trail reached the end of the track and there, resting on the sandy bottom, left an impres- sion of the outline of some marginally relatively rigid structure of the ventral surface. Had the organism started out from this oval area, it is obvious that the oval would have been partly effaced and merged into the trail. The complete adjustment of the oval terminal impressions to the trails thus becomes of extreme interest; for it must be that in these impressions there is a clue to the outline of the organism which produced Climac- tichnites. The larger of the terminal impressions measured at Bidwell’s crossing gave a length of 16 inches and a breadth of 6G inches. The oval impressions are somewhat more depressed in the sand than the trails, particularly toward the posterior margin of the impressions [see plate A to the right of the knife]. In figure 1, a sketch is made of what was interpretcd to be the general outline of the marginal groove of the ov2i impressions; but, either because the impressing body was tilted posteriorly downward so that it did not make so broad an impression anteriorly or because it was wider posteriorly than anteriorly, most of the distinct impressions are rather more pointed anteriorly than is shown to be the case in the diagram. There is also a broad swell in the center of the impressions. In the study of the forms which was made in the field, no traces of appendages or other ventral structures were made out. We are thus left to the trails, to the outline of the creature, and to the broadly undulating impression of the ventral surface to infer- its nature. REPORT O} YHE STATE PALEONTOLOGIST 1902 QG65. Comparison with the Chitons. Professor Walter Faxon sug gested to me, on secing the drawing, figure 1, a comparison of the oval impressics.s with the outline of the ventral surface of the shell of the modern larger Chitons. Some of the Chitons are somewhat narrower anteriorly than posteriorly; but the oval grooved impression which their ventral surface would: give has much resemblance to that of the sedentary impression of Climactichnites. The mantle of the Chitons extends beyond. the shells; they have a powerful foot for attachment to rock surfaces; though habitually attached to rock surfaces, they can. crawl very slowly over sand; they can roll themselves up into. a ball, as did many trilobites; the retractile forward hitching movements of the foot of a large Chiton, moving inch by inch, might have given rise to the smoothened, cross-ridged trails known as Climactichnites; and the sedentary animal with re- tracted foot, the terminal impressions seen at Mooers. No other existing form seems so readily capable of producing the assem-. blage of phenomena. But it is equally possible that some large. sea slug of the order of Aplacophora may have produced the trails and the terminal impression, though the modern repre- sentatives of these primitive gastropods are not littoral ani- mals. Further than the suggestion of a molluscan origin for these terminal impressions and the connected trails, it does not seem possible at present to seek definite conclusions. It is. possible that a more detailed study of the terminal impressions at Mooers with proper illumination will bring out faint traces of impressions not here described, and that from these diagnos- tic characters may be obtained. The sedentary impressions terminate the history recorded by the trails. What became of the animal after making the seden-- tary impression is a matter of conjecture. A jellyfish or a naked mollusk such as Doris, becoming stranded, may wither away, leaving no recognizable vestige of its substance; this would hardly be the case with the Polyplacophora. It may be sup- posed that the animals which made: the sedentary impressions. on the Potsdam sandstones at Mooers fioated away with the incoming tide. On the other hand, it is quite unlikely that in: ’ the porous sandstones of this area — for porous. they. must haye- 966 NEW YORK STATE MUSEUM ~ been a long time after their deposition —the shell structure of a mollusk would remain to the present time. The manner in which several of the trails approach in a common direction and end close to each other in sedentary im- pressions is exactly what takes place in the case of the trails of many gregarious aqueous forms, which crawl up a béach or a partly exposed sand bar and rest on the dry sand. The pres- ence of the trails leading to the sedentary impressions is con- clusive proof that wave action was not concerned here in strand- ing the animals. The modern limulus, for instance, in the breeding season during the month of May on the Massachusetts coast, comes ashore in shallow bays, several individuals crowd- | ing the shore at the same place. The difference in the size of the terminal impressions and the convergence of the trails at Mooers | suggest that more than one individual was concerned in mak- ing the trails here described. Other occurrences of Climactichnites noted in 1902. Small partly effaced trails of Climactichnites were seen on the glaciated sur- face of the Potsdam sandstone in the road gutter on top of Covey hill, in Canada, about two miles west of the Covey Hill post- office. The sandstone is exposed there for a long distance in the trenches on either side of the road. These tracks were seen on the north of the road. A drifted block of Potsdam sandstone carrying narrow, straight, cross-ridged Climactichnite trails without a central ridge was found on the Mooers quadrangle near the Chazy river in the longitude of Irona N. Y. This specimen was sent to the State Museum. 94} JO UOI}Isod oy} YyavUT D OF V S19}}9, [BIIdEO OT, I 93¥[d WO USATS SUOI}O_S ’ J “eluBA[ASUUegd PUG YLOX MON Ul AUTOIA S}I puw PeSSNOSIp o19Y VOIY oy} Jo deuI yoyS WINDAIASNN 3d MNOLINIAg! Net NSYuuM 5.5; RESNNOL NII MM Va HLYUON ABIVAIA IWIASLHSIYND Sa a7TONBH>O Jaeny JIIWMNASNOLNG. YOA KA3BN aN MATSONUY PB one yuyl= "22 ] 317V9S role le DEVONIC AND CARBONIC FORMATIONS OF SOUTH- WESTERN NEW YORK With stratigraphic map of the Olean quadrangle BY L. C. GLENN INTRODUCTION Basis of paper. During the summer of 1900 the detailed geolo- gic mapping of the Olean and Salamanca quadrangles in south- western New York [see pl. 1] was undertaken by the United States Geological Survey in cooperation with the New York State Paleontologist, and the writer was placed in charge of the work. The work was continued and finished the next summer. Mr Myron L. Fuller assisted largely in the work on the Salamanca quad- rangle during the latter season, and in both seasons Mr Charles Butts made extensive paleontologic collections from the two quadrangles and the adjacent region. Reconnaissance work was pushed southward to Bingham Pa. and westward across McKean and Warren counties to near Corry Pa. Age of rocks and problems involved. The paleozoic rocks ex- posed in the quadrangle extend from about the middle of the Chemung up into the Carbonic. They consequently include the Catskill or its equivalent and the boundary or transition be- tween the Devonic and the Carbonic. Eastward in both New York and Pennsylvania the distribution of the Chemung, the Catskill and the Carbonic rocks and their relationship to each other have received much study. Southward in Pennsylvania the Carbonic rocks have been studied and the lower Carbonic traced northward toward this region. To the west in Ohio the Carbonic and Waverly have been studied and traced eastward for some distance into northwestern Pennsylvania. The Olean- Salamanca region, however, has been an unknown meeting ground into which, when attempts were made to trace beds that were distinct to the east, the south or the west, the tracings became indistinct and the correlations uncertain. Purpose of paper. It is the main purpose of this paper to de- scribe briefly the stratigraphic succession found in the Olean- Salamanca region, to state the paleontologic conclusions so far reached as to the age of the formations, and the results of the efforts made to trace these formations into better known re- 968 NEW YORK STATE MUSEUM gions southward and westward in McKean and Warren counties Pennsylvania. - Topography. Topographically the region is a maturely dis- sected one. The hills rise with steep slopes to an elevation of 500 to 1000 feet above the main stream levels. The northern portion of the two quadrangles is glaciated and exposures of rock in place are infrequent. Much of the southern portion and of the reconnaissance area in Pennsylvania is wild and wooded, and overgrown in many places with a dense tangle of bushes, briers and vines that both conceals exposures and ren- ders the work of the geologist difficult and slow. Structure. The dominant structure is that of flat lying beds dipping gently a little west of south at. an average rate of about 30 feet a mile. Here and there the dip is locally increased or decreased and in the Olean and eastern Salamanca area just south of the Allegheny river it is for a short distance reversed. Some sharp minor folding occurs in the Olean conglomerate south of Olean along the high ridge extending from Flatiron rock to Knapp’s creek and beyond. This folding is entirely taken up in the 1800 feet of shales that intervene between the Olean conglomerate and the Bradford oil sand which is pene- trated by many wells at this depth and shows no sign of folding. In the Salamanca region some low rolls or folds with northeast- southwest axes were noted by Mr Fuller. STRATIGRAPHY _ DEVONIC FORMATIONS Chemung’ beds Description of Chemung shales and of Cuba sandstone lentil. The oldest rocks in the region are those near stream level in the northeastern part of the Olean quadrangle. They are typical Chemung shales and extend upward some 700 to 750 feet. Of these the very lowest beds consist of 30 or 40 feet of fine olive- green, argillaceous shale, seen best exposed in railway and other cuttings near Cuba. An excellent exposure may be seen a few yards east of the Erie depot at Cuba. In the railway cut 20 feet of it are exposed and nearly 20 feet more may be seen in the gutter by the side of the street leading down into the town. It is here fine grained and weathers into very small fragments. REPORT OF THE STATE PALEONTOLOGIST 1902 969 When fresh the lower part is bluish in color and the upper part green, but it weathers to a rusty brown from its iron content. It is sparingly fossiliferous. Immediately above these shalcs there is a sandstone 10 to 15 feet thick, most prominently exposed in and north of Cuba in a number of quarry openings. It is a medium to coarse grained, somewhat: arkosic sandstone, usually of a light cream- eolor and smelling strongly of petroleum on freshly fractured surfaces. As seen in a quarry a few rods east of the Erie depot in Cuba there are exposed at the base 8 feet of thick bedded, hard, cream-colored sandstone, above them two feet of green and brownish shale, then two feet of sandstone abundantly fossilif- erous. Above these are about 12 feet of sandy olive shale that weathers to a rusty brown, then 2 feet of thin-bedded flaggy sandstone, above which are seen to the top of the opening 8 feet of interbedded shales and thin shaly sandstone plates. The lower 10 feet of the sandstone are quarried. In places the stone is stained with iron along joints and seams. Fossils occur rather abundantly in certain layers and in the coarser parts an occasional small quartz pebble is found. Other quarry openings are found in and near Cuba. At North Cuba the rock has been opened at several places and probably furnished the stone for the dam of the old canal reservoir there. The region in which it occurs above water level is glaciated and almost all outcrops are concealed by till. It extends from North Cuba and Ischua, however, down Oil and Ischua creeks to near their junction where its dip carries it beneath flood plain level. A solitary exposure of sandstone having the same general appearance, situated at about the same geologic horizon, and carrying the same characteristic Cuba sandstone fossils is found in a Buffalo, Rochester and Pittsburg Railway cut north of Great Valley on the Salamanca quadrangle and has been correlated with the Cuba sandstone. All other exposures along Great Valley creek are entirely concealed by the drift so that its areal extent there is unknown. From its exposure in quarries in and around Cuba this sand- stone is known as the Cuba sandstone. It is regarded as a lentil in the Chemung formation. 970 NEW YORK STATE MUSEUM Above the Cuba sandstone lentil the Chemung is composed of green and brownish argillaceous and sandy shales, inter- bedded here and there with thin shaly sandstones. With the probable exception of certain dark purplish shales to be described presently, the individual beds of neither the shales nor the shaly sandstones usually retain their. thickness or individuality or possess any lithologic character that would enable any one of them to be traced and identified for any dis- tance. The nearest approach to persistency in these variable beds is found in a sandy zone about 200 feet above the Cuba sandstone. A number of quarries have been opened in the past on some argillaceous sandstones at this horizon. The stone is fine grained and soft and is more accurately described perhaps, as a shaly sandstone that varies into an indurated mudstone. When exposed to the weather the outside scales off or cracks and seams develop, so that in each quarry opened it was soon found to lack durability. All these quarries are abandoned today but at intervals along either valley wall of Oil and Olean creeks from one a few miles above Hinsdale that furnished material for locks for the old state canal te ones to the west and to the south of Olean may be jseen the old openings. But even this sandy zone, persistent as it is as a whole, well illustrates the variability in detail of these Chemung strata for often in one quarry face there is visible a complete change along the bedding plane from one lithologie phase to another, so that as a whole these Chemung shales and argillaceous sandstones are only regular in their irregularity and intergradation. | The one exception as regards the rapid variability of these shales is found in certain dark purple or chocolate colored shales about 325 to 350 feet below the top of the Chemung. These are largely sandy and interbedded with thin plates of very shaly sandstone often of about the same color. They sometimes have a reddish cast but it is always a very dark brick red never a bright red. They seem to be widely persistent and are found in many well borings to the south. Their top occurs in the Dennis well at Bradford Pa. at a depth of 712 feet. In a few places south of Cuba some faint traces of oolitic iron ore are found in the shales a hundred feet or more above REPORT OF THE STATE PALEONTOLOGIST 1902 971 the Cuba sandstone. They seem to be of local development and even in this region are scarcely worth mentioning. Ata number of horizons the shales become locally caleareous and a bed 6, 8, or even 10 inches thick may pass into a very impure limestone that where exposed on the surface has usually been leached out into a honeycombed mass of brachiopod casts and molds. These thin beds weather into: soft rusty blocks or ehunks that are often very conspicuous on the surface. In many places the sandy shales and thin shaly sandstones, specially near the top of the Chemung, are stained bluish black by manganese. Ripple markings are common at various horizons and in a few places what may possibly be obscure mud eracks are found. Minute mica scales often fleck the parting planes of the thin shaly argillaceous sandstones. As a rule the Chemung strata are abundantly fossiliferous. Brachiopods and lamellibranchs are the most abundant forms while in some ef the abandoned quarries above mentioned sponges are also to be found. Cattaraugus beds Wolf creek conglomerate lentil. A marked change in the con- ditions of sedimentation caused the deposition of a conglom- erate that is most prominently developed on Wolf creek and is known as the Wolf creek conglomerate. Its pebbles are predominantly flat or discoidal and hence it is also often called the “flat pebble” conglomerate in contradistinction to the Olean or “round pebble” conglomerate occurring higher in the series. The pebbles are mostly of vein quartz though a few are of red jasper. They vary in size from an inch or two in diameter down to ones of coffee or wheat grain size. Pebbles of the larger size are not abundant. The average size is per- haps less than a half inch in diameter. The mass of the rock is as a rule a coarse, loosely cemented, cross bedded sand sometimes bleached white but usually stained yellow or brown by iron. In some places on Wolf creek it becomes locally massive, and projects from the valley walls in ledges 15 to 20 feet high from which large blocks are shed into the valley below. One of the most prominent characteristics of this conglomerate is its rapid_variation in thickness. Nowhere more than about 20 feet thick, it often in a few hundred yards thins 972 NEW YORK STATE MUSEUM down to a few inches in thickness. It was at first thought that these thicker portions might mark an old stream channel but a careful mapping of them failed to reveal any relation to a possible stream course. Notwithstanding its rapid variation in thickness it was found to be a remarkably persistent stratum over the Olean and the eastern part of the Salamanca sheet and was the key rock for determining the stratigraphy of much of this region. Its maximum thickness of about 20 feet is found in only a few localities and these are on Wolf creek. Elsewhere in the Wolf creek region it is frequently found 5 to 10 feet thick, but over by far the larger part of the area in which it is known to occur in these two quadrangles it is only from a few inches to a foot or two thick and consequently is not a conspicuous stratum and is rarely exposed in a natural outcrop. Its horizon in numerous places is determinable only by tracing up a hillside loose pieces on the surface to the highest point at which they can be found and then working along at this elevation till the upper limit of loose material is well established. Even in a part of the region where it is, as a rule, very inconspicuous it may for a short distance thicken materially, as for instance northeast of Carrollton where it is locally 10 or 12 feet thick, and it is entirely possible that in the portion of the Salamanca quadrangle where it is not known to occur and where its horizon is indicated by the dotted geologic boundary line between the Chemung and the Cattarau- gus there may be here and there spots where a few inches or a few feet of it are to be found. The beds occasionally contain a fair to good representation of marine fossils the assemblage of which is characteristic of this horizon. It marks the first prom- inent change in sedimentary conditions in the region and is re- garded as a lentil marking the base of, and belonging to, the Cattaraugus formation. Shales and sandstones. The deposition of the Wolf creek con- glomerate was succeeded by conditions that caused the deposition of bright red shales interbedded with green or blnish shales and fine grained, greenish gray, thin bedded, micaceous sandstones that together extend upward through an average interval of 300 to 350 feet. This portion of the stratigraphic column in which bright red shales occur, and REPORT OF THE STATE PALEONTOLOGIST 1902 973 which extends upward from the base of the Wolf creek con- glomerate lentil in the Olean region to a limonitic shale pres- ently to be characterized, is regarded as a formation and to it the name Cattaraugus is given. Two other conglomerate lentils occur in it, the Salamanca and the Kilbuck. | The bright red argillaceous shales of the Cattaraugus are entirely different from the dark brick red or purplish shales of _ the Chemung and need never be confused with them. No bright red shales occur anywhere in this region below the Wolf creek conglomerate but they do appear within a few feet above it. They are usually fine grained and argillaceous though in many places they become sandy and may locally pass into a thin red argillaceous sandstone. Specially does this transition occur in the southeastern part of the Olean area and in eastern McKean county, Pa. It is not certain that the individual beds ef red shale are persistent or hold their thickness for more than short distances, but it is certain that as one goes west- ward into the Salamanca region and southwestward into War- ren county, Pa. the beds of red shale tend to disappear. Their disappearance appears to be due not to a lack of deposition in this area at that time, nor to their once having been depos- ited and subsequently removed from the entire region by erosion before the deposition of the overlying formations but to their grading over westward and southwestward into deposits of other than red color. The stratigraphic equivalents of the red shales are as a rule present to the westward but their color has changed to olive-green, blue or drab. At the same time there is some evidence that erosion occurred in this region after the deposition of the beds containing these red shales as will be seen somewhat later. The lighter colored shales interbedded with the red ones vary from fine blue mud shales to light or dark green sandy ones. Along with the shales are greenish gray, medium to fine grained, soft, arkosic sandstones often thin or cross bedded and with their parting planes fiecked with mica particles. By the oxidation of their iron content these sandstones weather ito a red soil just as the red shales do. These sandstones have been quarried and sawed into flagging at the Cook quarry a few miles south of Olean, though no work is now being done 974 NEW YORK STATE MUSEUM at this place. The individual beds of sandstone do not seem to be persistent except for short distances. There is found, however, in a number of places in the Olean region a rust- colored sandstone layer filled with limonitic concretions and containing fish remains, but whether these exposures belong to one persistent horizon or not is uncertain. To the southwest near Warren Pa. fish remains are known to occur at several horizons. Fossils. After the deposition of the Wolf creek conglomerate which contains in its upper portion specially a marine fauna, fossils rapidly disappear and the red and green shales and the fine micaceous sandstones generally yield but few or, for con- siderable intervals, no forms. In many places, specially in the sandstones, fossils are entirely wanting. Conditions as a whole were evidently unfavorable to animal life while these beds were being deposited. Some fish remains occur as mentioned above and the Salamanca and Kilbuck conglomerate lentils are fossiliferous. — | Salamanca conglomerate lentil. The Salamanca lentil occurs at about the middle of the Cattaraugus formation. It thins out and disappears to the eastward, not being known to occur on the Olean quadrangle to the northeast of the Allegheny river and Oswayo creek. South and west of this line it occurs in the Olean area ag a hard gray sandstone 10 to 15 feet thick, which becomes coarser and thicker westward and passes into a massive conglomerate on the Salamanca quadrangle. The sandstone phase is well exposed in a number of small quarries on Mount Hermon just south of Olean where it is locally known as the Mount Hermon sandstone. It is there a medium to a coarse grained sandstone carrying an occasional small quartz pebble. It is generally cream-colored to gray though some layers are dotted with innumerable small rust-colored spots that have — resulted from the decomposition of iron pyrite. The bedding here is usually regular and the thickness of a given bed uni- form for at least some distance. The layers of from 8 to 16 inches in thickness are separated by thin shale films or partings that render their removal easy. It weathers into hard, white, parallel-sided blocks that are pierced by many vertical fucoid tubes or stems. These fucoids are often very prominent and are REPORT OF THE STATE PALEONTOLOGIST 1902 975 a characteristic feature of the weathered blocks in the Olean region. Its massive conglomeritic character is best developed in the Salamanca region and may be well seen up Limestone and Irish brooks, along Red House creek, at Salamanca rock city where it weathers into great blocks, and at numerous other places. In thickness, coarseness and massiveness it is also variable though not as markedly or abruptly so as the Wolf creek. In its more massive phase it is often strongly cross bedded and in places is separated into two benches with a shale parting be- tween. The pebbles are mostly of vein quartz and the great majority of them are distinctly flattened like those of the Wolf creek and, like the latter also, they include an occasional one of red jasper. Even when coarsest and most massive the peb- bles do not appear as prominent or form as large a proportion of the mass as they do in the Olean conglomerate. The bulk of the rock consists of a-coarse, gritty sand. The average size of the pebbles is small and they are usually distributed through the mass of the rock not uniformly but in thin streaks along the planes of the cross bedding. The difference between the flatness of the pebbles of the Wolf creek, the Salamanca, the) Kilbuck and the two thin con- glomerates just below the Olean and the roundness of the peb- bles of the Olean itself was first noticed by Carll! whose ex- planation of their flatness as due to beach action would seem to be correct. He regarded older shore deposits lying to the north as the source of the pebbly materials. As the presence of the occasional jasper pebbles among the flattened quartz ones in all of the conglomerate beds in the region below the Olean or round pebble conglomerate gives suffi- cient gounds for concluding, it is believed by the writer that the coarse materials of these lower, or flat pebble conglom- erates, were derived from the Lake Superior region and were transported eastward along the shore by the waves and long shore currents of the Devonic and Carbonic seas, the flat- tened or discoid form so characteristic of the pebbles of these lower conglomerates being produced by their to and fro mo- tion along the beach during this long eastward journey. Carll, J. F. Geol. Sur. Pa. Rep’t I,, p. 60, 61; I4, p. 190-92 976 NEW YORK STATE MUSEUM The round or ovoid pebbles of the Olean conglomerate which ‘contains no jasper pebbles, it is further believed were not trans- ported along the beach but were brought down from the ancient land masses to the north and east and were rolled over and over and rounded by the stream currents that carried them into the Carbonic sea. The flattened pebbles were beach fashioned, the rounded ones stream made. The total maximum thickness in the Olean-Salamanca region is rarely over 30 feet and probably © mever exceeds 40. Much confusion and uncertainty has arisen in the Salamanea region as to the number of conglomerates present beneath what has generally been called the Subolean. This is specially true of that region bordering the valley of the Tunangwant or Tuna. Various correlations, some of which, however, were recognized as provisional, have been made for the same outcrops, and dif- ferent outcrops of the same conglomerate have often been re- garded:as belonging to different horizons. ait The names Salamanca, Panama, Pope Hollow, Wrightsville and even Subolean (?) have all been applied in this region to the same conglomerate some of them being regarded by some as synonyms but the belief being prevalent that two or three conglomerates are present in the Tuna section. ‘Lesley for in- stance, believed there is lowest a Salamanca (Panama?) con- glomerate, above it a Tuna-Pope Hollow-Wrightsville conglomer- ate horizon and above that an Ireland-Subolean (?) one. J. F. Carll? believes that at least 225 feet above the Salamanca con- glomerate the Tuna occurs and is the equivalent of the Ireland Subolean (?) of Lesley and probably the equivalent of the Pope Hollow-Wrightsville conglomerate found farther west. F. A. Randall? recognizes in the Tuna region a lower or Panama and an upper or Pope Hollow conglomerate and thinks it probable that the Salamanea is the equivalent of the Pope Hollow. The lower conglomerate found by Randall northeast of Carrollton and up Baillett brook and perhaps in a few other neighboring localities is the Wolf creek here locally much thickened as com- 1Lesley, J.P. Geol. Sur.Pa. Summary Final Rep’t. 2:1531-32. ? Carll, J. F. Sec. Geol. Sur. Pa. Ia: 203-8. 3 Randall, F. A. Preliminary Report on Geology of Cattaraugus and Chau- tauqua Counties. N.Y. State Geologist An. Rep’t. 1893. p. 713-21. EE ——— se REPORT OF THE STATE PALEONTOLOGIST 1902 977 pared to its usual development in this region. His higher con- glomerate is the Salamanca. The Salamanca, the Panama, the Pope Hollow and the Tuna are the same conglomerate and Lesley’s supposed third or Subolean(?) conglomerate at Ireland near the head of Irish brook is also an excellent outcrop of the Salamanca, here quite massive. The confusion has mainly resulted from assuming a regular dip for the Salamanca and then concluding that a conglomerate found too high or too low at a given locality for the calculated position of the Salamanca at that place belonged to a different horizon. Dips, however, are not regular in this region. A local northward reversal of dip occurs near the mouth of the Tuna and again just southeast.of Salamanca and several small rolls or gentle irregular folds with northeast southwest axes occur in the Salamanca area. These irregu- larities render such dip calculations misleading. Kilbuck conglomerate lentil. On the Salamanca sheet there is found in the Cattaraugus formation a third conglomerate lentil lying 50 to 70 feet above the Salamanca conglomerate and called by Mr Fuller the Kilbuck. It has much the same flat peb- ble character as the underlying Salamanca. It is not over 10 to 15 feet thick as a maximum but in places is quite massive and weathers into large flat blocks that, where topographic con- ditions favor, form a pavement over considerable areas. It is best developed northeast and east of Kilbuck and extends as far east as the ridge at the head of Tenmile creek. It is also found north of Salamanca and on the high ridge south of Sala- manca and east of Red House brook as far south as the head of Irish brook. A small area occurs on the ridge east of the Tuna and north of the head of Leonard brook. It is thus seen to be of local development, but has possibly added to the difficulties of making correct correlations in this region. Probable unconformity. The top of the Cattaraugus formation. is difficult to determine with exactness in most places since its. upper portion consists of soft shales and it is succeeded by other soft shales. Exposures are in consequence poor except along roadways or pipe lines. Numerous measures, however, that are deemed reliable have been obtained of the thickness. of that part of the formation which lies above the top of the. 978 NEW YCRK STATE MUSEUM Salamanca conglomerate lentil. A comparison of these figures shows that this thickness frequently varies irregularly and very materially within short distances. The interval from the top of the Salamanca to the top of the Cattaraugus near Flat- iron is 65 feet, southwest of Knapp’s creek it is about 145 feet. In the Dennis well at Bradford Pa. it is 84 feet. At the head of Chipmunk creek it is about 90 feet. East of Chipmunk it is 110 feet in one place and in another near by more than 145 feet. At the head of Leonard brook it is 180 feet, northward at the head of Baillett brook it is 220 feet, while still north beyond the Allegheny it is only 100 feet on the knob east of Carrollton. In several places in the Limestone-Irish brook region it is 100 feet or less while just north of Rice brook it | is at least 230 feet. On the southeast side of upper Red House brook it is 110 feet while on the northwest side it is over 210 feet. At the triangulation station southeast of Salamanca it is 215 feet or less, a mile and a half north it is 240 feet or more. It is not thought probable that mere local variations in the thickness of the strata of the Cattaraugus could be rapid enough and great enough to account for the irregular varia- tions that have just been mentioned in the thickness of that part of this formation which lies above the Salamanca con- glomerate lentil. It seems more probable that the upper surface of the Cattaraugus is irregular because of erosion and that there is consequently an unconformity at this point repre- senting an erosion interval between the Cattaraugus and the succeeding Oswayo. | 3 CARBONIC FORMATIONS . Oswayo beds Composition. The close of the Cattaraugus stage was marked by the cessation of the deposition of red shales in this region. After what is believed to have been an erosion interval it was followed by the deposition of olive-green to rusty colored sandy shales, with here and there thin sandstone layers with limonitic seams or incrustations. These greenish, limonitic shales constitute the Oswayo formation. Its thickness varies from 160 to 250 feet, the average being near the latter number. Conditions now became more favorable to the existence of life and, in contrast to the usual barrenness of the red shales REPORT OF THE STATE PALEONTOLOGIST 1902 979 below, the Oswayo contains in many places a fairly good repre- sentation of marine invertebrates, prominent among which is Camarotoechia allegania, which serves as an excel- lent horizon-marker. Limestone layer. A few feet above the base of the Oswayo shale is found in a number of places in New York what seems to be a persistent layer of very impure limestone. It is only one or two feet thick and in places is separated into two layers with several feet of shale between. This limestone is com- posed of innumerable fragments of badly broken brachiopod and other marine shells. It might almost be termed a shell conglomerate. In places it also includes: bryozoan remains. One of the best exposures is seen in an abandoned railway cut at the burned power-house on the electric road about a mile north of Olean rock city. It is again found just off the Sala- manca quadrangle on both the present and the abandoned line of the electric road southwest of Knapp’s creek in several places. Near the head of Nichols run on the hill southeast of Limestone and at the head of the western branch of Red House brook along an abandoned railway grade just beyond the edge of the Salamanca quadrangle it is again found. It is probably the same as a very similar limestone which the writer has examined at a number of places in McKean county, Pa. and which is called by Ashburner! the Marvin creek limestone with the suggestion that it is probably the same as the Lower Mead- ville limestone of Crawford county. On the Olean quadrangle a few small areas of Oswayo shales are found on the highest crests north and east of Portville, but they are mainly found on the highest ridges south of the Alle- gheny river and in this region extend up to the base of the Olean conglomerate. Near their top they become sandier and the number of thin limonitic sandstone plates increases. On the Salamanca quadrangle the largest areas of Oswayo shales aré found south of the Allegheny river. They occur on almost every prominent ridge. North of the river the only areas of any size are those on the ridge crests on either side of Tenmile creek. | — ——— ee 1Ashburner, C. A. Sec. Geol. Sur. Pa. Rep’t R, p. 68-69. 980 NEW YORK STATE MUSEUM At Olean rock city there are some traces of grits some forty or more feet below the base of the Olean conglomerate. WNo- where on this quadrangle, however, have such gritty beds been found exposed in place and at several points good exposures of — this part of the section are to be seen, as for instance on the road from Fourmile down into Fourmile creek valley. The trace of grit at the rock city may be the equivalent of one or the other — probably the lower — of the two thin conglom- erate beds found interbedded with shales and lying just beneath the Olean conglomerate westward at Knapp’s creek and else- where on the Salamanca quadrangle, and which will presently be described. If so, these coarser beds have so fined down and lost their characteristics that it becomes impossible to separate them on the Olean quadrangle from the Oswayo shales beneath and both are on this quadrangle accordingly mapped together under the name of the Oswayo. It is very probable that over most of the small area on the Olean quadrangle where the upper part of the Oswayo shale occurs the very topmost beds, which are the equivalent of the grits and interbedded shales westward, were eroded before the deposition of the Olean and consequently that even if this part were lithologically separable from the Oswayo there would be very little of it to map. Knapp beds On the Salamanca quadrangle there are found beneath the Olean conglomerate two thin conglomerates interbedded with shales that are lithologically very similar to the underlying Oswayo shales. These are doubtless in part at least the equiva- lents of the grits and shales just beneath the Olean at rock city and which are included in the Oswayo there but which evidently thicken and coarsen westward till they are capable of differ- entiation as the Knapp formation. These beds are not usually well developed on the Salamanca quadrangle and have been found in only a few areas along the southern edge. Southwest- ward in Pennsylvania a more prominent conglomerate known as the Subolean is situated in a similar stratigraphic position be neath the Olean from which it is separated by from 25 to 50 feet of shales. It is known over a large area and extends according to the Pennsylvania geologists westward into Ohio where it is REPORT OF THE STATE PALEONTOLOGIST 1902 981 known as the Shenango conglomerate. It with the associated Shenango shales is probably the equivalent of this Knapp formation. | | f The coarser part of this formation is usually a loosely ce- mented conglomerate with small well smoothed quartz pebbles of flattened discoidal shape that only in places becomes massive. It is frequently highly limonitic and in most places where exam- ined was fossiliferous. The fossils consist of marine inverte- brates and plant stems of various kinds. The shales are sandy and ojive-green or rusty brown and in several places have been found to contain marine invertebrates. | The most eastern exposure of these beds is found at Knapp’s Creek Station. Here there are two coarse beds separated by a varying thickness of shale. In the gutter beside the road lead- ing from Knapp’s Creek Station down into the head of Fourmile creek, in the interval from 20 to 40 feet below the station level, is found a thin bedded gritty to pebbly sandstone heavily charged with iron and containing marine invertebrate fossils. The layers are separated by partings of blue clay shales. A few hundred vards west of the station along the electric road just before reaching the summit there is a second sandstone about 40 feet higher than the first one, the interval between being occupied by sandy ferruginous shales. This sandstone is hard and gray and rings under the hammer. It is bedded in layers _a few inches thick, some of which contain a few pebbles. The layers are separated by ferruginous sandy shales. It is also fossiliferous bearing among other forms Syringothyris. Above it are perhaps 20 feet of shale before the base of the Olean is reached. Beyond the summit one passes down through the Same succession in reverse order, the upper sandstone being about 5 feet thick and more conglomeritic, the underlying shale being 20 feet thick and the lower coarse bed consisting of 20 feet of thin conglomerate and sandstone interbedded with shale, the pebbles being chiefly of wheat grain to coffee grain size. Both beds are again fossiliferous. These beds—specially - the upper one — are found exposed at intervals along the ridge westward nearly to Harrisburg. At Harrisburg and to the northwest they have been cut out and several small areas of 982 NEW YORK STATE MUSEUM Olean conglomerate lie at a lower elevation than these underly- ing beds do just to the south and east. _ The best development of this formation in the Salamanea quadrangle is found on the ridge southwest of Limestone near the Pennsylvania line. These two thin conglomerates again occur just beneath the Olean. They are very well exposed along the pipe line crossing this ridge. Each is more massive and more conglomeritic than in the Knapp’s creek area. The upper one at least is fossiliferous. They are each 10 to 15 feet thick. The shale interval between varies from 30 to 40 feet in thick- ness and is fossiliferous, containing among other forms Syringo- thyris again. There are about 25 or 30 feet of shale between the upper conglomerate and the base of the Olean. Farther . south and west only one conglomerate known as the Subolean has been seen by the writer beneath the Olean and the shale interval is usually great enough to make it seem most probable that this one conglomerate is the lower of the two in the above — mentioned localities, if both have not united westward. In some other places also these beds seem to have been cut out by erosion before the deposition of the Olean conglom- erate, as, for instance, on the ridge north of the head of Irish brook, where Olean caps the hill but with no sign of an under- lying conglomerate beneath. The same thing is true at Miller’s cliff in Warren county, Pa., where the Olean occurs, but beneath it the Subolean is wanting. There is consequently believed to be an unconformity between the Olean and the underlying formations in this region and from differences of level in the base of the Olean as exposed in outcrops often but short distances apart, the floor upon which the Olean was deposited must have been a very irregular one. PPotteqille pede Olean conglomerate. Next comes a massive round pebbled conglomerate widely known as the Olean conglomerate. In texture the Olean often varies quite rapidly both horizontally and vertically. In some places or in some beds it is scarcely more than a coarse sandstone with a sparing development of pebbles, while at other places or in other layers at the same place, it is almost entirely composed of rounded quartz pebbles. If any rule holds good the lower part is more frequently con- REPORT OF THE STATE PALEONTOLOGIST 1902 983 glomeritic and the upper part a coarse, cream-colored sand- stone that weathers white on exposure. It is almost always strongly cross bedded. The pebbles are well rounded and in contrast to the flattened or discoidal pebbles of all of the under- lying conglomerates in the region are predominantly ovoid in shape so that the Olean is frequently referred to as the “round pebble conglomerate.” While flat pebbles do occur in it, yet the proportion of round or ovoid ones is so great that the distinction is good. These pebbles vary in size up to two or three inches in diameter though the average diameter is some- what less. Most of them are of vein quartz; a few are of a hard, dark gray slate; none are of red jasper. They are loosely embedded in a very arkosic sandy matrix, in portions of which there is considerable iron which has formed thin limonitic streaks or crusts through the rock and resists disintegration much better than the arkosic cement does. Etched quartz pebbles. Pebbles of vein quartz embedded in surfaces made of such limonitic crusts are frequently found much etched or corroded. The only part played by the limonitic crust is the holding of the same pebbles exposed on its surface for some time till the etching agent has had time to greatly corrode them. The nature of the etching agent is not certainly known. It is generally thought to be some one of the humic acids that result from plant decay. The best examples of such etching seen in the region by the writer are in shallow depressions in which water stands after a rain on the upper surface of the blocks that make up the Genesee rock city. These huge blocks are on the top of a high crest in a field with only one tree near that rises above them. The upper surface of the blocks is bare except for a very few submicroscopic plant forms which may possibly by their decay furnish a corroding agent, though this impressed the writer when examining them as not being an adequate cause. The next best example of etching is found at Olean rock city. Here both the cause and one rather diagnostic step in the process seem more satisfactorily determinable. On the under surface of overhanging portions of the rock so situated — 984 NEW YORK STATE MUSEUM that they could not be wet by rain or receive drippings from any surface above were found many small well etched pebbles of vein quartz. These under surfaces of the rock were very appreciably moist, however, even on a hot summer day. This moisture was derived partly by seepage of contained moisture down through the loosely cemented rock itself and partly by direct condensation of moisture from the atmosphere, since from their sheltered position these surfaces remain quite cool even on the hottest days. If due to an organic acid of decompo- sition, this acid must have reached the etched under surface by soaking through some 30 or 40 feet at least or rock. Why it has not attacked and corroded the many quartz pebbles passed on its way through the rock, but has preferred to wait - till it has reached the under surface before becoming chemically active seems explicable on the theory advanced by Dr C. Ww. Hayes. The acid was probably humic and so was compara- tively inert till it had come into free contact with the atmosphere on reaching the underside of the ledge, where it © absorbed nitrogen from the air forming azohumic acid which has a strong affinity for silica and at once began corroding the quartz pebbles. These somewhat exceptional conditions at — Olean rock city seem most readily explicable on this theory and they in turn lend additional strength to the theory itself. Disintegration of the Olean is as a rule very rapid and talus slopes occur everywhere so that the base is rarely or never exposed. Numerous well borings have penetrated it, however, on the Olean quadrangle and give an accurate measure of its thickness there which is usually between 60 and 70 feet, though in one well it is 90 feet. It occurs on the highest hilltops in the southern part of the two quadrangles, in a number of small detached areas and is well known southward in McKean county and westward in Warren county in Pennsylvania. 3 Above the Olean conglomerate at rock city are found a few feet of thin, sandy, ferruginous shales in which some years ago a thin coal bloom was exposed in grading a road. It also belongs to the Pottsville. 1 Hayes, C. W. Solution of Silica under Atmospheric Conditions. Geol. Soc. Amer. Bul. 8:213-20. ar REPORT OF THE STATE PALEONTOLOGIST 1902 985 AGE OF FORMATIONS Paleontologic work. The extensive collections of fossils made by Mr Charles Butts were studied by him at Albany under Dr J. M. Clarke’s supervision. Prof. H. S. Williams has also studied similar collections made some years ago by himself and his assistants in this region and the paleontologic facts stated below concerning faunal affinities are those ascertained as a re- sult of the investigations of Dr Clarke, Dr Williams and Mr Butts. Additional facts bearing on the paleontologic problems of the region may soon be expected as a result of the further studies now in progress by Drs Clarke and Williams. The conclusions which the writer has drawn from these paleontologic facts he alone is to be held responsible for. The shales extending from the lowest exposures up to the base of the Wolf creek conglomerate contain an abundant Chemung fauna and are considered to be of Chemung age. The first Car- bonic life forms appear with the incoming of the Wolf creek con- glomerate and from this point up to practically the base of the Olean conglomerate at Olean rock city where the last Devonic forms disappear, there is a mingling of Devonic and Carbonie _ forms, the Devonic slowly decreasing, the Carbonic slowly in- creasing. The essential fact so far as the life of these Catta- raugus and Oswayo formations is concerned is that there is an overlapping of Devonic and Carbonic faunas. With this essen- tial fact recognized the position at which the boundary line between the Devonic and the Carbonic shall be drawn becomes, in some measure at least, a matter of convention. It might appear best for some reasons to draw this line at the base of the Wolf creek where Carbonic forms first appear and consider both the Cattaraugus red beds and the Oswayo and Knapp formations as Lower Carbonic. This would make the top of the Chemung the top of the Devonic and would make the Subcarbonic average about 600 feet thick in this region. Because of the thickness of these red beds and their reason- ably certain stratigraphic equivalence with the red beds of the Catskill to the east, and because of the unconformity believed to exist between the Cattaraugus and the Oswayo, the writer pre- fers to draw a provisional boundary between the Devonic and the Carbonic at this point. This would make the Subcarbonic 986 NEW YORK STATE MUSEUM 300 to 350 feet thick here and would make the top of the red beds the top of the Devonic. All of the facts bearing on this difficult Devono-Carbonie boundary problem will not be at hand till paleontologic re- searches from both the Devonic and Carbonic starting points have been finished and detailed stratigraphic work has been carried eastward, southward and westward to connect with bet- ter known and more clearly differentiated areas in these direc- tions. Hence this boundary is to be recognized and accepted as distinctly provisional only and is subject to such change .as later investigations of the stratigraphy and paleontology of the adjacent regions may warrant. The Olean has been agreed on as Carbonic but there has been | considerable difference of opinion as to just what portion of the | Carbonic it represents, though the weight of opinion has been in favor of its age being Pottsville. Very recent field studies by Messrs M. R. Campbell! and David White are regarded by them as definitely establishing its Pottsville age. It is still doubtful, however, as to what part of the Pottsville it repre- sents. It may be the equivalent of either the Connoquenessing or of the Sharon. If it be equivalent to the Sharon, the few feet of overlying shale represent the Sharon shale and the thin coal bloom the upper Marshburg coal. If it be the Connoquenessing, the overlying shale and coal belong to the Alton or Mercer coal group. Detailed work to the south and west will be necessary to settle this point. RECONNAISSANCE A reconnaissance was made southward into McKean county, Pa. and then westward on both sides of the state line pee to the western edge of Warren county, Pa. Wolf creek conglomerate. South of Ceres the Wolf creek con- glomerate is well developed along King’s run, being in places fully 20 feet thick but weathering into pieces a few inches to a few feet thick. It dips under stream level a short distance north of Glenn postoffice. West of this point on the road to Eldred it appears at the upper fork of Newel creek and is again seen on the road just south of the upper fork of Barden brook, whence it may be traced to Eldred where it outcrops 120 feet ~ 1 Personal letters from Mr M. R. Campbell, Ap. 18 and 27, 1903. REPORT OF THE STATE PALEONTOLOGIST 1902 987 above railway level. It is represented in the Dennis well at Bradford by part or all of the 35 feet of sandstone with base at 1620 feet above tide. West of Bradford it is not satisfactorily identified. It probably loses its character even as a sandstone ‘and soon entirely disappears westward. Salamanca conglomerate. No traces of the Salamanca conglom- erate were found south of Ceres or near Eldred. In the Dennis well at Bradford it is represented by the 28 feet of sandstone with “a few pebbles,” having its base at 1817 feet above tide. West of Bradford it is found up Marilla creek and west of Marilla summit it occurs on Corydon creek. It is again found west of the Allegheny river both in Pennsylvania and south of Steamburg in New York and from its elevation, its position in the section and its lithologic character as well as by its tracing westward, the writer concludes that it is the same as the Pope Hollow conglomerate, which may be traced south from Pope Hollow past Fentonville and Russellsburg by exposures at inter: vals along either valley wall of the Conewango to the Asylum quarry at North Warren. It may be traced westward up Rhind’s run by numerous exposures to a point on Jackson’s run about 2 miles east of Chandlers Valley. All exposures from here to Sugar Grove are covered with glacial till but it is quar- ried a short distance west of Sugar Grove, is found just above the mouth of the Lottsville well no. 1! and may be traced at intervals along the Little Brokenstraw valley northward past Grant station till there can be no doubt of its being the Panama conglomerate. Tracing it southward from Lottsville it passes about 225 feet beneath the Wrightsville conglomerate at Wrightsville and is doubtless the pebbly sandstone found “about 100’ from the surface ” in the Rocky Hollow well? about a mile northeast of Wrightsville. It seems probable that far- ther south this Salamanca-Pope— Hollow-Panama conglomer- ate may be the same as the third Venango oil sand if that sand has a northward representative at all. . In this northwestern part of Warren county the shales and thin soft micaceous sandstones that extend for a couple of hun- dred feet above the Panama conglomerate weather into a steep Carll, J. F. Se. Geol. Sur. Pa. Rep’t I4, p. 199, 232. "Carll, J. F. Sec. Geol. Sur. Pa. Rep’t Jy, p. 236. a O88 NEW YORK STATE MUSE""M but smooth slope that is highly characteristic and bears when cleared, as it usually is, a characteristic -vegetation. These Shales with their characteristic topography and vegetation often aided in tracing the underlying Panama where it was not ex- posed or had even dipped somewhat beneath drainage level. Wrightsville conglomerate. The Wrightsville conglomerate can not be identified with the Panama, but lies about 225 feet higher in the section. It seems reasonable to suppose that it is the equivalent of the Venango first sand as is believed by Lesley, though no attempt was made by the writer to trace it to a connection with that sand.t Olean and Subolean conglomerates. The Olean conglomerate is found on Mount Raub near Bradford and occurs on the hills south of Bradford decreasing gradually in elevation till it is last exposed in the Buffalo, Rochester and Pittsburg Railway cut just north of Bingham station as an irregularly bedded sandstone. Here it dips under the plateau surface. No exam- ination was made of the region south of the divide where it doubtless reappears. The Olean conglomerate and the She- nango conglomerate and shale are traceable westward across Warren county. All occur on Quaker hill and at Pike’s rocks and elsewhere. The Olean appears at Miller’s rock but the ~ Shenango seems to have been cut out there just as its equiva- lent, the Knapp formation, has been near the head of Irish brook and elsewhere as previously noted. 3 Local pebble beds. During the reconnaissance lecally devel- oped pebbly beds usually only a few inches in thickness were — found at several points. These thin pebbly beds occupy no definite horizon but apparently may occur anywhere in the Cattaraugus or Oswayo formations. In no case was any one of them found to be persistent or to possess any stratigraphic importance. They were revealed by chance in some unusually good exposure in a railway cutting by the roadside, or along a stream bank and would ordinarily have entirely escaped observation. It is possible that at some point in the region 1For the opinions of the geologists of the second Pennsylvania survey on the correlations of the various members mentioned in the preceding paragraphs see White, I. C., Report Qs, p. 99-116; Carll, J. F., Report Is, p. 57-80, I4, p. 195-208, - v. 304-8 (F. A. Randall); Lesley, J. P., Summary Final Rep’t, 2: 1493-1536. rr. ee a io 2 REPORT OF ‘THE STATE PALEONTOLOGIST 1902 989 such a pebbly bed may thicken into a locally prominent stratum ~and become a source of perplexity and possible error in tracing the stratigraphy if no near-by measure to a known horizon were obtainable as a check. Fucoids. Fucoidal remains in the shape of vertical tubes piercing the sandstone or conglomerate layers of the Salamanca are specially characteristic of that horizon and in its north- eastern portion were often used as an aid in its identification, though in all cases of doubt reliance was placed in its inverte- brate fauna. Southwestward in Warren county, Pa. while vertical fucoidal remains are still often very prominent in the Salamanca, they also occur at other horizons and hence if they may be used at all in that region as an aid in identification, it must be done only with a recognition of this fact in mind. COLUMNAR SECTIONS A few columnar sections selected at considerable intervals over the region are added in order to give some idea of the general stratigraphic succession in the region. They are ne- cessarily generalized somewhat in the representation of thin beds. The concealed intervals are in most cases almost cer- tainly shales but in the sections are left blank. In section C pieces of the Wolf creek were found loose on the surface up to the level indicated by the displaced blocks, and the same thing is true of the Salamanca in section E. The thickness of the two thin limestone layers in the basal part of the Oswayo in section F is much exaggerated. In some cases the interval represented as being red shale consists of red and green shales interbedded in very thin layers. The purple or chocolate col- ored shale beds of the Chemung are seen in sections B and D. Eastward from B the Salamanca conglomerate lenses out, and in B the Subolean conglomerate —-though probably not con- glomeritic in this particular section— had been eroded before the deposition of the Olean. Finally, the writer wishes the conclusions that have been reached as to correlations in McKean and Warren counties to — be recognized as ones based on a reconnaissance in a region where such work is beset with many difficulties. It is believed, however, that detailed work will only confirm the conclusions reached. ai E UNIVERSITY OF THE STATE OF NEW YORK, John M. Clarke, State Paleontologist. ANNUAL REPORT, 1902 STRATIGRAPHIC MAP OF THE REGION ABOUT UNION SPRINGS AND PART OF THE CITY OF AUBURN CAYUGA COUNTY LEGEND Onondaga limestone Rondout waterlime Cobleskill lim: Geology by J. M. Clarke and D. D. Luther. Scale aztoo The Argus Co. State Printers L 3 ° 1 2Miles —— ——— = Bt Ey ° a 2Glometers Contour interval 20 feet, Danan is mean sea level, FOSSIL FAUNAS OF THE OLEAN QUADRANGLE BY CHARLES BUTTS In pursuance of instructions received from the state paleon- tologist, the fullest possible collections of fossils were made from nearly every fossil-bearing outcrop on the quadrangle, including 259 stations. The analysis of the fossil faunas thus collected reveals their distribution according to the accompany- ing lists and seems to warrant the division of the strata into several zones, whose positions in the general stratigraphic succession are exhibited in the following columnar section. A few feet of shale exposed in the deeper valleys near the north- ern margin of the quadrangle are not shown in the section, as no collections were made from it. : These zones correspond with Mr Glenn’s divisions as follows: Zone 2 is the Olean conglomerate, zone 3 is the, Oswayo shales and Knapp beds, zone 4 is the limestone layer, zone 5 is the interval between the limestone layer and the top of the Sala- manca conglomerate, zone 6 is the Salamanca conglomerate, zone 7 is the interval between the Salamanca and Wolf creek con- glomerates, zone 8 is the Wolf creek conglomerate, zone 9 is the interval between the Wolf creek conglomerate and the top of — the chocolate shales, zone 10 is the chocolate shales and the quarry sandstones, zone 11 is the interval between the quarry layer and the Cuba sandstone, and zone 12 is the latter. bed. On comparison of the zonal lists, it appears that there is a gradual disappearance of species on passing upward through the strata without the appearance of any new elements till the horizon of the Wolf creek conglomerate is reached. The zones below this horizon are therefore based on this disappearance of species at certain horizons, which gives rise to a slightly different facies to the overlying fauna. The zones do not coin- cide with the vertical range of some one or more characteristic. species having definite upper and lower limits. Thus, so far as my collections show, Orthothetes chemungensis does not pass above the top of no. 11, Athyris angelica disappears at the top of no. 10, while at the top of no. 9 all but nine species disappear, and their places are taken in the next zone, the Wolf creek conglomerate, by new genera and species. € REPORT OF THE STATE PALEONTOLOGIST 1902 991 This important faunal change with the incoming of the Wolf creek conglomerate, taken in connection with the fact that on stratigraphic grounds, the equivalent of the Waverly of Ohio, of Subcarbonic age, is pretty certainly present in this quad- rangle, and in connection with the fact that the fauna of the conglomerate and higher beds contains a small Subcarbonic ele- ment, would indicate that the bed might be provisionally adopted as the base of the Subcarbonic in the quadrangle. Of the 128 species collected, 60 species occur below the Wolf creek conglomerate only, 59 species occur above the same horizon only, and nine are common. Of the 59 species occurring above the conglomerate, seven species can be referred to the Lower Carbonic. These are Ctenodus flabelliformis, Gyracanthus sherwoodi, Oehlertella pleurites, Orthothetes crenistria, Glossites (Sanguino- lites) amygdalinus?, Sphenotus aeolus? and Crenipecten winchelli. The stratigraphic significance of the abundant Ptychopteria fauna, so highly characteristic of zones § and 7, is not fully understood, as its stratigraphic rela- tionships have not been fully worked out. It must be admitted that the positive evidence is scanty and in itself hardly sufficient to establish a boundary line between the Devonic and Carbonic at the base of the Wolf creek conglomerate, but in a case like this, where the stratigraphic evidence warrants the conclusion that such a boundary line exists, this evidence seems sufficient to give it a provisional location. Further than this it would be hardly safe to go. If this location be not accepted, there seems to be no paleontologic ground for such a boundary line at all below the Olean conglomerate. Of the remaining zones, no. 5 is almost hae of fossils, no. 4 is a thin limestone in which Camarotoechia allegania Williams, makes its advent. This species is specially abundant in no. 3 and highly characteristic of it. A few fragmenitary re- mains of a Camarotoechia and an obscure pelecypod or two were found in fragments of Olean conglomerate, hitherto supposed to be nonfossiliferous. The species of fossils found in and below the Wolf creek con- glomerate are all marine. The presence of Holoptychius and Bothriolepis scales in no. 7 would indicate fresh or brackish \ 992 NEW YORK STATE MUSEUM water deposits, but, in the midst of these, thin layers of ferru- ginous conglomeritic sandstones or lumpy mud rock bearing marine fossils occur. No fossils of any kind are found in the red shales of no. 7 and 5. The fossils from the top of no. 7 to the top of the section are all marine with the possible exception of some obscure impressions of plant stems, some of which appear to be calamites, occurring at the top of the Olean conglomerate. . | The most favorable localities for collecting in zones no. 11 and 12 are found in the quarries and ravines at Cuba and vicinity and near the mouths of streams entering Ischua creek from Hinsdale to Ischua. In the other zones the best exposures occur and the best opportunities for collecting are found in the quarries and railroad cuttings both north and south of Olean. The Wolf creek conglomerate however has yielded fossils only in loose material in the vicinity of Portville on Wolf creek and on the high hills in the northeastern part of Cuba township. LIST OF SPECIES SHOWING ZONAL DISTRIBUTIONS DEVONIC ; Chemung beds | Zone 12, Cuba sandstone lentil (base of section) Spirifer disjunctus Sowerby Orthothetes chemungensis Conrad — S. mesacostalis Hall Productella lachrymosa Hall Athyris angelica Hall Schizodus rhombeus Hall Camarotoechia contracta Hall Grammysia communis Hall Orthis (Schizophoria) impressa Hall Zone 11 Spirifer disjunctus Sowerby | Aviculopecten ? Hall Athyris angelica Hall | A. eancellatus Hall A. cora Hall ' | A, rugaestriatus Hall Camarotoechia contracta Hall AS Spa C. duplicata Hall Crenipecten crenulatus Hall Chonetes scitulus Hall Edmondia subovata Hall Orthis (Schizophoria) tioga Hall K. phillipi Hall O. (S.) leonensis Hall E. obliqua Hall Cryptonella sp. ? Leptodesma potens Hail Orthothetes chemungensis Conrad» L. potens var. juvens Hall Productella lachrymosa Hall ( L. mortoni Hall P. costatula Hall L. sociale Hall P. onusta Hall L. longispinum ? Hail P. speciosa Hall L. protextum‘?-Hall > _ me Se Tl REPORT OF THE STATE PALEONTOLOGIST 1902 L. spinigerum Hall? Lyriopecten cj. anomiiformis Hall Macrodon chemungensis Hail Modiomorpha quadrula ? Hall Nucula cf. bellistriata Hall Palaeoneilo brevis Hall Pterinopecten crenicostatus Hall _ P. neptunus Hall 993 Sphenotus clavulus Hall S. sp. ? Grammysia subarcuata Hall Orthoceras sp. ? Cyclonema sp. ? Kuomphalus hecale Hall Macrochilus sp. ? Dictyospongia sp. ? Zone 10 Spirifer disjunctus Sowerby Athyris angelica Hall Camarotoechia contracta Hall Chonetes scitulus Hall ~ Lingula sp. ? Orthis (Schizophoria) leonensis Hall O. (S.) tioga Hall Productella lachrymosa Hall Aviculopecten tenuis Hall A. duplicatus ? Hall A. sp. ? Crenipecten crenulatus Hail Edmondia phillipi Hall Leptodesma potens Hall L. potens var. juvens Hall L. mortoni Hall L. sociale Hall Mytilarca chemungensis (Conrad) Hall - Nucula ? Pteronites ? Ptychopteria ? Pterinopecten crenicostatus /Zull P. neptunus Hall Schizodus sp. _ Sphenotus clavulus Hall S. contractus Hall S.. sp. ? S: spo? Grammysia subarcuata Hall Orthoceras sp. ? Bellerophon maera Hall Cyclonema ? Euomphalus hecale Hall Straparollus sp. ? Prismodictya choanea Hall & Clarke P. prismatica Hall Thysanodictya poecilus? Hall & Clarke T. edwin-halli Hall & Clarke Zone9 ~ Spirifer disjunctus Sowerby Camarotoechia contracta Hall C. contracta var. robusta Butts C. sappho ? Chonetes scitulus Hall Orthis (Schizophoria) tioga Hall Productella lachrymosa Hall _ Aviculopecten sp. ? Edmondia subovata Hall Leptodesma potens Hall L. mortoni Hall i L. sociale Hall L. sp. ? Modiomorpha quadrula Hall Nucula ? Ptychopteria elongata Hall Spathella ? Sphenotus clavulus Hall S. contractus Hall Sa, Speie Straparollus sp. ? Arenicolites DEVONO-CARBONIC Cattaraugus formation Zone 8, Wolf creek conglomerate lentil Spirifer disjunctus Sowerby Camarotoechia contracta Hall - Lingule m Leptodesma orodes Hall Modiola praecedens Hall ~ 994 NEW YORK STATE MUSEUM P. proto Hall | Schizodus sp. ? P. salamanea Hail | Sphenotus clavulus Hall P. elongata Hall _ Gomphoceras sp. ? Palaeanatina typa Hall | Orthoceras sp. ? Zone 7 Spirifer disjunctus Sowerby | Schizodus rhombeus ? Hall Camarotoechia contracta Hall Sphenotus clavulus Hall Lingula sp. ? S. cf. arcuatus Hall Oehlertella pleurites Meek Grammysia sp. ? Orthothetes crenistria,? Phillips Orthoceras sp. ? Aviculopecten patulus Hall Bellerophon sp ? = Leptodesma sp. ? Straparollus sp. ? -Modiola praecedens Hall Tropidocyclus ? Ptychopteria sp. ? Strophostylus ? P. proto Hall Bothriolepis minor ? P. salamanca Hall B. sp. ? Po spi? Ctenodus flabelliformis Newberry P. elongata ? Hall Holoptychius americanus Palaeanatina typa Hall Gyracanthus sherwoodi Newberry P. solenoides Hall - Lone 6, Salamanca conglomerate lentil Spirifer disjunctus Sowerby Allerisma ? n. sp. Camarotoechia contracta Hall | Ptychopteria proto Hall C.sappho Hall. P. salamanca Hall Crenipecten winchelli Meek He cyan. t Leptodesma orodes Hall | P. elongata ? Hall L. curvatum Hall | Palaeanatina typa Hall L. macluri Hall Schizodus chemungensis var. quadran- rsp? gularis Hall Modiola praecedens Hall Sasp: | Pararca transversa Hall ‘Sphenotus aeolus Hall P. elliptica Hall Orthoceras sp. ? P. transversa Hall Straparollus sp. ? Zone 5 Ptychopteria perlata ? Hall S. contractus Hall Pterinopecten suborbicularis ? Hall Orthoceras sp. ? = Sphenotus clavulus Hall Agelacrinites buttsi Clarke SUBCARBONIC Oswayo formation Zone 4, limestone lentil : disjunctus Sowerby | Camarotoechia allegania Williams REPORT OF THE STATE PALEONTOLOGIST 1902 995 Zone 3, Oswayo shales and Knapp beds Pugnax ? sp. ? Lingula sp.? Syringothyris randalli Simpson Rhynchospira scania Hall& Clarke Bryozoan gen. and sp. ? Spirifer disjunctus Sowerby Athyris polita Hall Camarotoechia allegania Williams C. sappho Hall Oehlertella pleurites Meek Orthothetes cf. crenistria Phillips Aviculopecten ? eS Dt pararca transversa Hall Mytilarca simplex Hall Grammysia c/. hannibalensis Shumard Allerisma ? 2, sp. nov. ? Palaeanatina typa Hall Schizodus chemungensis ? Hall Orthoceras sp.? Leptodesma orodes Hall L. curvatum Hall L. maclurii Hall esp. ? L. mytiliforme Liopteria sp. ? Ptychopteria sp. ? CARBONIC Zone 2, Olean conglomerate Camar®®echia cf. allegania Williams Ptychopteria ? | Sphenotus contractus ? CONSTRUCTION OF THE OLEAN ROCK SECTION BY JOUN M. CLARKE The differing interpretations of the Olean section given by Professor Glenn and Mr Butts in the papers preceding, afford an excellent illustration of the discrepancy which often resuits from the two modes employed. This discrepancy pertains how- ever solely to the determination. of a conventional boundary plane in sediments characterized by the uniformity of their succession. The sequence of events involves the independent construction _ of the lithologic or purely stratigraphic evidence and of the facts derived from the succession of faunas. In a great thickness of arenaceous sediments carrying variable intermixture of clay, slight and oft recurring differences of texture are produced and these variations are so locally related to coastal contour and bathymetry, to tidal ebb and flow and to stream discharge, that sedimentary differences seldom hold true far away from a given section. In the Upper Devonic of New York this marine arenace- ous sedimentation prevails through a thickness of 2500 to 3000 feet. It has long been a subject of close study. By the con- struction of a large number of meridional sections from east to west through the lower or Portage division of this sedimenta- tion we believe that we have now arrived at an understanding of the proper correlation of sections which, in the actual suc- cession of sediments, differ fundamentally. Doubtless with the similarly close analysis of the Chemung beds we shall arrive at an equally clear understanding of the succession and lateral extension of sedimentary differences. If we have gained any lesson from the careful analysis of these earlier or Portage sedi- ments and their contents it is this, that in these shallow water deposits there is very little correspondence between the sedi- ments and the organisms that lived on them, that indubitably - continuous sediments may carry, without necessary variation of texture, wholly different organic combinations at different places; that faunas shift, encroach on the provinces of others | and retreat without concomitant change in the sedimentation. Hence a history of the events of sedimentation from which may be drawn the record of coastal alterations, of shifting coast lines and bars, and, in consequence of increased or lessened terrestrial a ) a en as a REPOR' OF THE STATE PALEONTOLOGIST 1902 997 erosion, does not correspond with exactitude to the succession of events recorded by the dissemination of faunas and their internal changes of composition. Perhaps no more effective illustration of the discrepancy in these standards of classification could be brought forward than that of the Portage sandstone, an element in this series of arena- ceous deposits —a well marked stratum which at -the east of this region contains a highly developed Chemung fauna, but westward carries no Chemung species whatever and still farther west changes its lithologic texture also. Some hundreds of feet of sediment under it in the east likewise carry a brachiopod fauna, while in the west that fauna is wholly replaced in equiva- lent and continuous strata. We could not therefore portray on -amap the succession of faunas for the Portage or lower belt of these arenaceous strata, so that there would be any correspond- ence to a cartographic portrayal of the succession. of sediments. So far as we now understand the Olean and Salamanca regions after the careful survey on which Professor Glenn has reported and from a long standing previous acquaintance with the rocks and their contents, it may be said that there is less probability of discrepancy in the deductions derivable from independent. con- sideration of the stratigraphic and the paleontologic evidence be- cause the uniformity of sedimentation is unaccompanied by so pronounced differences in faunation. The most serious question involved in this survey so far as concerns the classification of the rock formations, is the con- struction of the Cattaraugus beds, the mass of chiefly red shales and sands with their included conglomerate lenses. To indicate the transitional character of these beds by employing as a pro- vistonal designation Devono-Carbonic, as was at one time sug- gested, is on the whole a makeshift satisfactory to no one. Hence Professor Glenn has preferred to admit them, for the time being, into the Devonic and to place the line of division between that and the Carbonic system at the top of these red Cattaraugus beds. It seems important however to take note of the two considera- tions through which this provisional determination is reached: (1) a possible unconformity at the top of the Cattaraugus beds, (2) the assumption of continuity of these red beds with the 998 NEW YORK STATE MUSEUM Catskill sediments of eastern New York and the tacit concession of the Devonic age of the entire series of those deposits. With regard to the phenomena interpreted as evidence of unconformity I should not be disposed to contest Professor Glenn’s inferences but to emphasize the fact that these sand reefs constantly dis- play indications of deep decapitation due to shifting of bars and change of direction of currents, or a modification by heavy tidal flow on a shelving coast. Unconformities thus frequently exist which are no indication of unrecorded time. As to the second assumption I feel that we should be specially cautious in taking for proven that Catskill sedimentation even in the typical sec- tion of the Catskill mountains is restricted to Devonic time. The Catskill represents a peculiar phase of sedimentation wide- spread in northern latitudes during the Devonic. The Devonic continent was profuse in great lakes and coastal lagoons whose sedimentation was carried on under conditions so unlike those of the ocean, that causes which would disturb and qualify the latter could not affect the former. We know that at certain places within the continental edge this sedimentation did con- tinue through the Devonic and endured till after the appear- ance of Carbonic faunas. Hence a certain part of Old Red sedimentation is in some instances postdevonic and may be so in New York; indeed in face of the paleontologic evidence I am very strongly of the conviction that it is so, and that the Cat- taraugus beds themselves supply the required proof of this fact. It is not a new suggestion that the upper stages of the typical Catskill are postdevonic; the restudy of this Catskill area which is now proceeding may give us new light on this point and though it would be the unexpected to find transgression of the Subcar- bonic fauna extending into this lagoon area so far to the east, by some other criteria it may be practicable to affirm this dis- tinction. Time must also elapse before assertions can be made as to whether the Catskill strata of eastern New York are or any part of them is continuous with the Cattaraugus beds of Allegany and Cattaraugus counties. : . The paleontologic evidence thus far derived from this section and summarized by Mr Butts, indicates one fact with emphasis, that is, the one substantial change in the succession of organic assemblages occurs with the incoming of the Wolf Creek con- REPORT OF THE STATE PALEONTOLOGIST 1902 999 glomerate, at the base of the Cattaraugus beds. Here Carbonic types appear, a new fauna is introduced and without attempt- ing to analyze again the time values of the various components (I have already discussed this point in my report of last year, op. cit. p. 524) it is enough to add that while the withdrawal of a large part of the Devonic fauna is concurrent with this new arrival, it is altogether to be expected that certain Devonic types survive. It will not do to state this condition as merely an intermixture of Carbonic and Devonic organisms, a charac- _ terization easily made and which would dismiss these beds as “transitional ” but it is rather the fact of a new arrival in the field while survivors of the old faunas or superstitial species still endure. The condition is normal for the process of replace- ment of one fauna by another. It matters little if among the superstitial species one remains so characteristic everywhere of the later Devonic as Spirifer disjunctus; for not alone in New York does this species transcend the limit of the Devonic and enter the Carbonic. With proper regard for such modifica- tions as additional evidence may require I am disposed to the conviction that in placing the dividing line between Devonic and Carbonic at the base of the Cattaraugus beds, as is done on the geologic map, we have the support of the most direct evidence. STRATIGRAPHY OF PORTAGE FORMATION BETWEEN THE GENESEE VALLEY AND LAKE ERIE BY D. DANA LUTHER With stratigraphic map Genesee valley The Portage formation received its name “ from its superior ‘development along the banks of the Genesee river in the dis- trict formerly included in the town of Nunda, now Portage,” Livingston co. The Genesee river is a northward-flowing stream, rising just over the Pennsylvania line and completely traversing the State to Lake Ontario. About 214 miles south of the north line of this town the valley through which the river has flowed northward for 50 miles or . more, ends, and the stream between ver- tical cliffs 200 feet in hight enters a nar- row rock gorge, plunges over three cascades ae respectively 76 feet, 110 feet and 66 feet high, with rapids above, below and between them, and descends about 350 feet in 2 miles, and 30 feet more to the north line of bie sy Portage township; so that, including 187 concretions feet of sandstone above the river at the upper end of the gorge and 75 feet for the Styliola | southward dip, about 635 feet of strata are exposed in the district referred to. The course of the river across the next town north, Mount Morris, is through a narrow canyon that broadens. out to a valley 14 to 14 mile wide, with steep banks and vertical cliffs from 100 feet to 250 feet high, and is about 6 miles long; this is fol- lowed northward by another canyon with Cashaqua shale black shale pyrite layer - Moscow shale Vartical cliffs, 150 feet to 300 feet high, On f . h ] e e e e ih Mgieaer to koproLeebole both sides, in which the river dashes from Lngstnne nd at pales side to side till the mouth of the gorge is reached at the village of Mount Morris, 11 miles in a straight line, and about 15 miles if the course of the river channel is fol- 2 Hall. Geol. N. Y. 4th Dist. 1843. \ REPORT OF THE STATE PALEONTOLOGIST 1902 1001 flowed, from the point where it crosses the Portage town line. - Jn this distance the river descends 100 feet, and the southward dip of the strata is 32.5 feet a mile. The Portage town line is 9 miles south of the mouth of the gorge at Mount Morris, and the dip therefore adds 292 feet to the thickness of the exposed strata and gives a total of 392 feet, of which all but 65 feet are included in the “ Portage group ” as described and himited by Prof. Hall. The Styliola or Genundewa limestone of the Genesee shales, which is 82 feet above the top of the Hamilton shales in the ravine of Little Beards creek at Lei- cester, 5 miles north of the mouth of the gorge, is exposed in the banks near the west end of the Western New York and Pennsylvania Railroad bridge at Mount Morris, and, with a few feet of black slates below it, is the lowest rock ex- posure on this section of the river. About 65 feet of typical upper Genesee shales overlie the Styliola limestone and are exposed at the east end of the cov- ered highway bridge at the mouth of the gorge, where the spheric concretions and characteristic fossils of this horizon are common. At the top of these bluish black shales there are a few lighter colored layers, some clayey, others slightly arenaceous, distributed through about 3 feet of Ree ee Fe yee parter shales. At-thig horizon. a-lighter. 0" sale. Stations 4, 5 band, hardly noticeable here, but fully developed farther east, has the sedimentary characteristics of the Portage shales and flags and contains a few fossils from both the mete and the Portage faunas. Overlying these passage beds there are 32 feet of densely black and bituminous slaty shales in which plant remains are light and dark shales with flags blue and black shale light shale black shale Cashaqua shale 1002 NEW YORK STATE MUSEUM common, and a few fish scales and plates have been found, but otherwise they are generally barren. A few small Lingulas (L.spatulata, L. ligea) found at the mouth of Pike creek on Lake Erie are the only fossils collected from this horizon, and they seem to belong to the species found in similar black shales higher in the formation. This bed_of black shales has quite the same structure and appearance as other black bands in the Portage section. Above this horizon there is no recurrence of the G'enesee fauna. The bottom of the passage beds immediately below the black band is therefore taken as the base of the Portage formation, and the stratum of black shales above has been designated by the state paleontologist as the Middlesex shales. . Middlesex black shales. This bed decreases slightly in thick- ness toward the west, but is thicker and quite arenaceous in the Dansville and Naples valleys. It is exposed in the cliffs on both sides of the Genesee river, from the mouth southward for a little more than two miles, the dip bringing it down to the water level on the south side of the “‘ Hogsback.” Near the top, after several alternations with lighter layers in a few feet, these shales are replaced by light bluish gray, and olive shales, “soft argillaceous rock of a green color” (Hall). Cashaqua shales. This mass is 165 feet thick, and was termed by Hall the Cashaqua shales because of their excellent exposure in detail in the gorge of Cashaqua creek, 5 miles east of the Genesee river. The general color of this shale in weathered exposures is a very light olive; but, when freshly excavated, it is medium dark bluish gray with frequent intercalations of darker or black layers of varying thickness, sometimes so thin and frequent as to give the rock a straticulate or laminated structure. In the section along Cashaqua creek there are a few thin flags in this horizon, and they increase in number toward the east. They are hardly noticeable in the Genesee river section. Uneven concretionary and more or less calcareous layers from 1 inch to 4 inches thick occur frequently, and some of them are continuous for many rods. Spheric and elongated concre- REPORT OF THE STATE PALEONTOLOGISS 1902 1003 tions from 1 inch to 1 foot in diameter are common throughout the mass, and appear in the rock wall at some horizons in well defined rows. é Fossils are not abundant in any part of these shales, but a few specimens occur in the lower part; they are much more common in the upper part, where they are found in con- ‘siderable numbers in a few thin layers of shale and also in the concretionary layers and the separate concretions. A row of concretions, usually a foot or more in diameter at the top of these shales and exposed in the river section, rests on a calcareous layer 1% inch to 2 inches thick that is composed of fossils, many of 7e=====4 sandstone which are finely preserved. This row of =e concretions is found at this horizon in — i nearly all the exposures of the shales from the Bristol valley, Ontario county ===) Table reck on the east, to the Tonawanda valley, = Naiee Wyoming county on the west. ——— It is exposed in the cliffs along the — Genesee river for about 3 miles and comes = ===! _ shales and | = fn down to the water level at the north end J _of Smoky hollow. ———— The passage from the Cashaqua shales ===] jiu shale to the next succeeding formation is through alternations of light and dark ” light shale shales, like those below, and the line of separation is therefore an arbitrary one. In the thickness given, 165 feet, nearly all of the transition layers at the top and bottom are included. Like the Hamilton, Genesee and the Middlesex shales, the Cashaqua shales thin toward the west, their thickness in the Lake Erie section being only 32 feet. In the Naples section Re at SAD OY farther east (Ontario county) there are Portage falls. Station 9 237 feet of shales and thin sandstones in this subdivision of the Portage formation. Alternate layers of black and gray shale overlie the fossilifer- ous concretions at the top of the Cashaqua beds to the thickness black shale i | i! lI black shale light shale black shale light shale 1004 NEW YORK STATE MUSEUM of 5 feet and are succeeded by 18 feet of black shale and 30 feet of dark and light shales in thin layers. Rhinestreet black shales. As the lighter shales decompose more rapidly than the black, the latter predominate in the coloring and, specially in old exposures, give to this division the appear- Pedy ance of being a homogenous bed of black : top of Upper shale. The division has therefore been z termed the Rhinestreet black shale from seniaeonse an exposure in the town of Naples. It is continuous from Yates county toe flags and Lake Erie, and, unlike all of the forma- tions below it down to the Onondaga ‘| sandstone limestone it increases in thickness . toward the west. wie It is 20 feet thick in the Naples sec- shales tion, 58 feet in the Genesee river cliffs and 185 feet in the Lake Erie section. Fossils are exceedingly rare in these dark shale black layers except terrestrial plant re- mains, which are found occasionally, drifted together and forming small thin layers of impure coal. Fish remains have been found in this horizon at plack shale Sparta, Livingston co., and other locali- Cepeceas ties toward the east, and a few speci- mens of Lingula and an abundance of conodont teeth have been obtained ieidle falls from it. RE cena 2 ‘This bed is exposed in the cliffs on the Middle Portage falls to abut- east side of Smoky hollow and at the Upper falls. Stations 10,11 falls in the outlet of Silver lake at Gib- sonville, also at the cascade in Buck run and on Cashaqua creek at Tuscarora. It is the base of “the great development of green and black slaty and sandy shales with thin layers of sand- stone” between the Cashaqua shales and the Portage sand- stones to which Professor Hall gave the name of ‘“ Gardeau shale and flagstones.” sandy shale shales and ags : 5S ! : q REPORT OF THE STATE PALEONTOLOGIST 1902 1005 The latter include 661 feet of strata exposed along that part of the river formerly in the Gardeau Indian reservation and to the top of the Upper falls at Portageville. Hatch flags and sands. Above the Rhinestreet shales are light and dark shales, 88 feet, in layers of varying thickness from a fraction of an inch to several feet, and with a few thin flags of fine blue sandstone distributed at irregular intervals. A row of Symmetric concretions, from 1 foot to 13 feet in diameter lies at the base of this subdivision, and many others of various sizes and shapes are seattered through it and serve to distinguish it from the overlying beds. Fossils are rare except in a few of the lighter layers, but the beds are more fossiliferous toward the east. Above there is a band of flaggy sandstones, 6 feet thick, ex- posed for several miles in the cliffs on’ the east side of Smoky hollow and the Gardeau fiats. It comes down to the river level opposite the “ Five Corners road,” 1 mile north of St Helena. At this point the cliff above the flaggy band shows 115 feet of shale in which no sandstones appear except about 10 feet of thin flags. A large proportion of this shale is dark and slaty, and the remainder is quite ferriferous, consequently the general aspect of the weathered face is very dark, almost black, and rusty. Fossils are almost entirely absent. — In the escarpment at the east end of the St Helena bridge 60 feet of these shales are exposed and are overlain by 25 feet of flags and soft sandstones that are separated from each other by thin layers of hard blue shale. This arenaceous bed is thicker and proportionately sandier toward the east. In the Dansville, Springwater and the Naples valleys it contains fossil sponges, and at the last place many brachiopods and other fossils, and marks the upper limit of the normal Portage fauna, and is there known as the Grimes sandstone. At the mouth of Wolf creek this bed is overlain by shales and flags 110 feet thick, in which dark or black shales still pre- dominate. It is exposed in the rock wall beneath the “ Table rock ” above the mouth of Wolf creek near the south road from St Helena to Castile, and in the gorge southward between the 1006 | NEW YORK STATE MUSEUM “Twin Hogsbacks ” to the Lower falls. It is seen also in the lower part of the Wolf creek ravine. | Fossils are very rare in it, but a few of the common Portage forms occur in the soft shales. | | Gardeau shales and flags. The layer of compact blue sand: ~ stone, 1 foot, 3 inches thick, that forms the “ Table rock” at the mouth of Wolf creek ravine, is the Same stratum as the “Table rock” at age the crest of the Lower Portage on the Genesee river. | : dark ae Above this mass lie 15 feet of soft oy light and dark shales and thin flags, at aoe the top of which is the hard even sand- : stone, 12 inches thick, that forms the dark shale crest of the low cascade at the head of ABE the Flume. Fossils are quite common in — blueand . the soft light shales between the two | as sandstone layers. py 8 soft light There are 49 feet of strata, mostly ars shales, between ‘Table rock” and the wth" horizon of the bottom of the Middle falls, concretions and 113 feet in the face of the Middle soft blue falls, in which there is a much larger te proportion of sandy layers. Fallen blocks of the sandstones from set te the vertical cliffs at and below the falls dark shales gyre almost entirely barren, but Aulopora and a few brachiopods, of species com- sandstone mon in thi§ horizon farther east, were shale found, but these probably came from black shale gome of the sandy layers above. | sandy shale There are 19 feet of flags and shales exposed between the top of the Middle and the horizon of the bottom of the Upper falls. Fic. 5 Section in the ra- vine at Wiscoy. Station 15 Fossils are quite common in a few of the soft layers of shale or shaly sandstone exposed between the Middle and Upper falls and to the base of the heavy sandstones above the Upper falls. They all belong to the Portage fauna, no brachiopods REPORT OF THE STATE PALEONTOLOGIST 1902 1007 being found among them. In the face of the Upper falls are 77 feet of flags and shales, and a layer of rather hard blue shale 4 feet thick exposed in the river bed for a few rods above the falls is takensas the top of the Gardeau shales and flags. In the 262 feet of strata between the “Table rock” and the top of the Gardeau beds, changes in the sedimentation are very frequent. Layers of black, blue black, blue gray and olive shales, and blue or olive sandstone, usually but a few inches thick, succeed each other in irregular order, but there is a noticeable increase upward in the sandy layers, and in the face of the Upper falls they equal or exceed the shales, though there are no heavy compact layers. Portage sandstones. The Portage sandstones consist of 187 feet of strata exposed in the walls of the gorge above the Upper falls, from the top of the 4 foot shaly layer at the crest to the top of the cliff on the east side south of the high railroad bridge. Except a bed of hard blue shale, containing calcareous nod- ules, 2 feet thick, 12 feet above the base and a layer of similar character 6 feet thick and 52 feet higher, the entire formation is com- posed of light bluish gray sandstone in layers from 2 feet to 10 feet thick, separated by 1% inch to 6 inches of shaly matter. In some of the upper layers the sand- stone is compact, durable and valuable for building purposes. Other layers are schistose along the laminae, and a few are shaly and friable. Large ob- scurely defined concretions occur in one or two of the more calcareous layers, but they are few. The two beds of shales and the shaly partings between the layers contain a very few fossils, all like those below. eee. In the sandstones Fucoides ver-_ ‘iffs. Station 13 ticalis is common, and plant remains occur, but otherwise they are practically barren here and along Wolf creek below flags shales flags and shale Sandstone with Chemung fossils -| dark shale flags 1008 NEW YORK STATE MUSEUM Long Beards riffs sandstone Wiscoy light and dark shales Portage sandstones Gardeau flags with shale Grimes — sandstone Rhinestreet black shale Cashaqua shale Middlesex shale Genesee upper shale Styliola limestone Genesee lower shale Fig. 7 Section on Genesee river from top of Hamilton at Moscow to Chemung sand- stone at. Jong Beards riffs, near Fillmore. Stations Oto 15 Hatch flags — Castile. They are exposed near the reser- voir on Quarry hill 1 mile south of Nunda, and a thin seam contains comminuted crinoids and brachiopod shells. In the Dansville and- Naples sections these beds contain an abundant Chemung fauna. 3 There is a small exposure of the sand- stones on the west side of the valley 1% miles south of Portageville, and the com- pact upper layers are quarried by the Genesee Blue Stone Co. 1 mile farther south. sae | The contact line between the sandstones and the succeeding formation is covered by drift in the immediate vicinity of the river, but a bed of black shales is exposed at Hunts Station on the east and 2 miles west from the high Portage bridge and along Wolf creek near Hopkins mill at Castile, the position of which is such as to show that the section exposed at Portage- ville practically includes‘all of the “ Port- age sandstones.” Wiscoy shales. The fossiliferous layers are exposed in. the north bank of the ravine of Wiscoy creek 14 mile above the village of Wiscoy, and below it are 157 feet of strata, many layers of which are black shales and others are soft, light colored and clayey. Small calcareous concretions are com- mon; and, except for the presence of a few thin sandstones, the entire formation be- tween the Portage sandstones below and the Long Beards riffs fossiliferous layer, so far as it is exposed, bears a close resem- blance to the Cashaqua shales, and the fossils bear a much closer relationship to the Portage fauna than to that of the Chemung rocks. REPORY’ OF THE STATE PALEONTOLOGIST 1902 1009 The Wiscoy shales are also exposed in Scotts ravine 2 miles northeast of Fillmore and in several other ravines on the east side of the valley opposite Rossburg. Naylor’s quarry near the Erie Railroad station at Castile shows a small section in the Wiscoy shales in which Manticoceras rhynchostoma is common at one hori- zon in the soft sandy shale. Toward the east the Wiscoy shales are more arenaceous, and the horizon is one of laminated or flaggy olive sandstones in which Chemung brachiopods are-abundant. Long Beards riffs sandstone. There are no rock exposures. along the river between the Genesee Bluestone Co.’s quarries and Long Beards riffs, 144 mile south of Fillmore, a distance of about 8 miles. © At this point an uneven layer of hard calcareous sandstone makes a low cascade in the river and is exposed on both sides of the channel. An escarpment on the east side of the riffs shows 10 feet of shales and flags below the principal layer, and 3.5 feet of Shales with a few even layers of sandstone above it. This heavy layer and another 4 inches thick 25 feet higher contain Chemung brachiopods abundantly. This horizon is the lowest in which Chemung brachiopods were found in place in the Genesee river section. Estimates based on such measurements as could be made, show it to be about 167 feet above the top of the “ Portage sandstones ” as exposed at Portageville. Résumé The Portage group, as exposed in the gorge of the Genesee river, which is the type section, includes between the top of the Shales bearing a distinctively Genesee fauna at the mouth of the gorge and the top of the Wiscoy shales at Long Beards riffs, 1207 feet of strata. | Marked changes in the character of the sedimentation make the following subdivisions of these beds recognizable, beginning at the base of the section: 1010 NEW YORK STATE MUSEUM ee 1 Passage “shales ar. cc tee, nec yc ocicn epi een ae ae 3 2 Middlesex ‘black ghale-.. 4750, to eee a 32 3: -Gashaquavshale, cence cau eee Shale tS hte Mee bree 165 4 Rhinestreet black shale.......... Oe eee ays) a dtatche alate mechs. eee ceecee anre ae Ue hee eee Bees f 203 6 -Grimes” SandStOme po isos os ee ree le 2.4 1 ‘Gardeau shales and aes... 02 oot eae eee 312 S POrlage SamdstOMes. cscs wos s = gees oe se ete ee eee 187 9). \Wiscoy Shale [Pies clit, oreo ocean eee 167 Totals .02. oF). PI9EL o Pe eee 1207 The following stations are localities where exposures of. these rocks are favorable for study. . i: Mouth of the gorge at Mount Morris. Formations exposed: the Styliola limestone, Upper Genesee shales, the transi- tion bed and the Middlesex shales of the Portage group. 114 miles south of the mouth of the gorge. The Middlesex shale and the base of the Cashaqua shale. . Lower part of the Buck run ravine, 14 mile east of Mount — Morris. The Cashaqua shale. | Upper part of the Buck run ravine. The Rhinestreet and the Hatch shales. North end of Smoky hollow, opposite the mouth of the Silver lake outlet. The Cashaqua, the Rhinestreet shales, and the Hatch shales and flags. Cliffs opposite the “Five Corners road” 1 mile north of St Helena. The Hatch flags. East end of bridge at St Helena. The Hatch ae and | the Grimes sandstone. | Cliffs and ravine at the mouth of Wolf creek. The Grimes sandstones, Gardeau shales and flags. Top of Lower falls. The Gardeau flags and shales. Top of Middle falls. The Gardeau flags and shales. Foot of Upper falls. The Gardeau beds. Sides of the gorge above the Upper falls. The Portage sandstones. rie Long Beards riffs, 1 mile south of Fillmore. Lowest sand- stones with Chemung fossils. i REPORT OF THE STATE PALEONTOLOGIST 1902 1011 15 Wiscoy creek ravine, above the bridge at Wiscoy. The Wiscoy shales, the Long Beards riffs sandstones and Chemung shales and sandstones. 20 Wolf creek ravine below Castile. The Portage sandstones and the lower part of the Wiscoy shales. 42 The ravine of Cashaqua creek from Son Yea to Tuscarora. The Cashaqua and Rhinestreet shales. Oatka valley section That part of the Oatka creek, or Warsaw valley, in which the bed rock belongs to the Portage formations, lies about 10 miles north and west, and 300 to 400 feet higher than the exposures of the same horizons in the Genesee river section, and is about 13 miles long. _ The Portage sandstones and the top of the Gardeau flags are exposed at Oatka falls near Rock Glen, but there are no other exposures of Portage strata in the channel of the river. There are many ravines, some of which are very deep, in the sides of the valley, and they afford good exposures, that together, vir- tually cover the entire Portage section. The following are some of the most important of the expos- ures, beginning at the north. ‘ In a small ravine on the west side, about opposite the village of Pearl Creek, the little brook flows over a cascade 15 feet high, of which a compact layer of the Styliola limestone of the Genesee shales forms the crest. Above the cascade about 50 feet of bluish upper Genesee shales are exposed, and a few feet of the Middlesex shales of the Portage formation outcrop above them, and rest directly on the Genesee shales. The transition bed is not perceptible here. In the ravine at Wyoming village about 50 feet of the upper _ part of the Cashaqua shales are exposed. They are mostly light bluish gray or olive and very soft. Calcareous concretions and concretionary layers are frequent. Fossils are quite common. Farther up the ravine and about 14 mile from the village, 40 feet of black shales in the horizon of the Rhinestreet shales are exposed, and above them, about 30 feet of alternate layers of light and dark or black shales. 1012 NEW YORK STATE MUSEUM The upper Cashaqua beds are also exposed along a small brook that comes into the valley on the east side 14 mile south of the Wyoming railroad station. In a ravine on the west side of the saadltavee 2 miles south of Wyoming, 150 feet of*the Hatch shales are exposed, and in an- other ravine about 2 miles farther south 120 feet of the strata next higher in the section. A flaggy band that occurs near the top of the exposure in the latter ravine is probably in the horizon of the Grimes sand- stones, but it is proportionately less arenaceous. In the Fall brook ravine 14 mile southwest of Warsaw there are 236 feet of shales and flags exposed below the Erie Railroad bridge. They are all in the horizon of the middle portion of the Gardeau beds, or that of the Lower and Middle falls at Portageville. Gibson’s glen is a ravine on the west side of the valley 21% miles south of Warsaw, that ends in a high fall, above which the basal layers of the Portage sandstones outcrop. About 150 feet of flags and shales are exposed below the sandstones. A thin layer of soft shale at the mouth of the glen contains many flattened concretions, in some of which finely ani fossils occur. A few fossils occur in all parts of the Gardeau division in this valley, but they are much more common near the bottom and toward the top than in the middle of it. In the ravine of Oatka creek, at and below the falls near Rock Glen, about 100 feet of Gardeau flags and shales are ex- posed and the lower layers of the Portage sandstones outcrop | along the stream above the falls. The old quarries of the Warsaw Bluestone Co. on the west | side of the Erie Railroad, near the village of Rock Glen, show | about 50 feet of the lower part of the Portage sandstones, and the upper part outcrops along the little brook southwest os the quarries. a REPORT OF THE STATE PALEONTOLOGIST 1902 1013 Stations in the Oatka valley 47 Ravine on west side opposite Pearl Creek. Exposed: lower Genesee shales, the Styliola limestone, the Upper Gene- see shales and the Middlesex shale of the Portage group. 48 Ravine on west side at Wyoming. ‘Fhe Cashaqua shales and the Rhinestreet shales. 49 Ravine on west side, 2 miles south of Wyoming. Bristol shales. 68 Ravine on west side, 214 miles north of Warsaw. Gardeau 7 beds. 45 Fall brook ravine 144 mile southwest from Warsaw. Gardeau beds. 46 Gibson’s glen, 2 miles south of Warsaw. Gardeau to base of Portage sandstone. | 69 Oatka falls near Rock glen. Gardeau to base of Portage sandstone. 70 Quarries of Warsaw Bluestone Co. at Rock Glen. The Portage sandstones. Tonawanda valley section The western part of Wyoming county and southeastern part of Erie county is an elevated region in which the higher ridges and hills are 1500 feet to 1700 feet A. T. It is in the drainage area of Lake Erie and the Niagara river, and the streams flow _toward the north and west, cutting a large number of valleys and deep ravines across the Portage rocks, in their rapid cescent cf 609 feet to 900 feet to the broad level area that borders the lake. The valley of Tonawanda creek is the most easterly one. It extends southward from Attica for about 10 miles, is 1%4 to 1 mile wide, and its sides are steep slopes, in which several small Streams have cut small gullies that expose the rocks. The rock section begins along the Tannery brook in the northern part of the village of Attica, where there is a long exposure of the upper Genesee shales. At the cascade 10 feet high, 14 mile above the old tannery, these light shales are succeeded by the black Middlesex shales. Te ee 1014 NEW YORK STATE MUSEUM The exposure continues a few rods up the stream, but the con- tact with the Cashaqua shales is covered. The Middlesex shales are also exposed in the bed of Tonawanda creek below the milldam in the village. The Tannery brook is crossed by the Erie Railroad 1 mile west of the village, and about 50 rods south of the railroad there is a.good exposure of the Cashaqua beds along the east branch of the stream. Fossils are quite abundant here in the shales and in the numerous concretions. The top of the Cashaqua shales and the lower part of the Rhinestreet shales are exposed a few rods farther south. A thin layer of pyritiferous black slate near the contact line contains Bactrites, Orthoceratites and a few other fossils — beautifully preserved in pyrite. = At Sierks station, 4 miles south of Attica, the upper part of the Rhinestreet shales is exposed in the bed and sides of Tona- _ wanda creek and the alternating layers of light and dark shales | of the base of the Hatch division on the hillside and along the — railroad south of the depot. Some fossiliferous layers of light — shale occur near the top of the exposed section and a row ot 3 large concretions a few feet above them. | At Varysburg, 8 miles south of Attica, there is am exposure of 25 feet of Gardeau flags and shales, with concretions and a few fossils, in the banks of Tonawanda creek, below the mill- dam in the village. With the exception of about 25. feet next above this exposure, that are covered, the Gardeau section may be seen in the bottom and sides of Stony brook, that comes in from the east through a deep ravine, and joins Tonawanda creek above the dam. This is a fine exposure, and it ends at the base of the Portage sandstones. | A small gully on the steep hillside west of Varysburg is crossed by the Buffalo, Attica and Arcade Railroad, at the altitude of 1240 feet A. T. Above the bridge about 250 feet of Gardeau flags and shales are exposed. A thin sandstone about level with the bridge contains fossil sponges. For 140 feet above this layer the beds are generally shaly, but flags and thin sand- - ’ 7 d REPORT OF THE STATE PALEONTOLOGIST 1902 1015 stones are frequent, and some of the shaly layers are quite sandy. A few of the sandstones are a foot or more thick and hard. The Portage sandstones are exposed in the upper part of the ravine to the brow of the hill. Some of the layers are compact and heavy and have the same appearance as in the Genesee river section, but most of the bed is softer and laminated, and | some parts are quite shaly. The thickness seems to be but about 75 feet, but the lower limit is not well defined. The bed of soft olive and black shales that succeeds the Portage sandstones is exposed above the crest of the hill in a short shallow gully. ; The Gardeau beds and the sandstones are also exposed in a similar ravine, 2 miles farther north, where the sandstones have © been quarried for railroad purposes. On the east branch of Tonawanda creek about 114 miles above the forks and 5 miles south of Varysburg, a layer of ‘ealcareous sandstone outcrops in the bed of the stream for a few rods, and the same stratum appears in a small quarry 4 mile northeast. It contains great numbers of small frag- ments of brachiopods, nearly all of which are too minute to allow identification of the species. It bears a very close resemblance to the Long Beards riffs fossiliferous layer; it is the lowest horizon in which brachio- pods were found in this section; as it is at the proper altitude, it is doubtless the same stratum, or, at least, in very nearly the same horizon. On the south side of the Erie railway bridge at Griswold, 6 miles west of Attica, the Styliola limestone is exposed in the bed of Murder creek. It is 18 feet above the top of the Hamil- ton beds as exposed in the east bank of the stream 50 rods north of the depot, and is overlain by 13 feet of typical upper Genesee shales, above which are the black Middlesex shales. A long flat exposure of the Cashaqua shales is in the bed and sides of the stream to the falls; including 5 feet of alternat- ing light and dark layers at the bottom and 12 feet of the same character at the top, they are 77 feet thick here. 1016 NEW YORK STATE MUSEUM At the falls and in the ravine above, about 100 feet of black Rhinestreet shales are exposed. A row of very large septaria, occurs in the black slates 28 feet above the top of the Cashaqua shales. The Middlesex shales and the base of the Cashaqua shales are exposed in the bed of Ellicotts creek, 144 miles west of the Erie Railroad station at Darien. The bottom of the Cashaqua shales is level with the rails on the bridge. This is the most northern exposure of Portage strata in this State. On Cayuga creek an outcrop at Iron Bridge Mills shows the — Styliola limestone and 12 feet of Upper Genesee blue black shales above it. ; At Cowlesville, 2144 miles south, there is a large exposure of the Cashaqua shales in the cliffs along the stream, and the Rhinestreet shales with many large septaria outcrop almost continuously below and above Folsomdale. At and above the forks at Cayuga creek,-3 miles south of Folsomdale, the top of the Rhinestreet shales and about 100 feet of blue shales, in which thin layers of black slates and a few flags are intercalated, are exposed. On Buffalo creek the upper part of the Cashaqua shales is exposed in the escarpment along the west side of the stream — below the bridge at East Elma. Fifteen feet of black slates crop out 114 miles up the stream, and at Porterville 100 feet of the Rhinestreet shales are exposed, in which two rows of very large septaria, separated by 35 feet of black slates, occur. Some of the septaria are 8 feet in diameter and 2 to 214 feet thick. At Johnson Falls, 7 miles up the valley southeast from Por- terville, a small creek comes into the valley from the east over a high cascade and through a short but deep ravine. There are 62 feet of Gardeau shales and flags exposed below the falls, and 144 feet in the face of the cascade and at the top. The beds are principally soft bluish shales with flags and thin sandstones, that are more frequent and thicker toward the — top. REPORT OF THE STATE PALEONTOLOGIST 1902 1017 The soft layers contain the common Portage fossils in small numbers, and crinoids and Aulopora also occur. : A layer of sandstone 2 feet thick, about 40 feet above the bottom of the cascades, contains fossil sponges. The horizon is very nearly the same as that in which sponges occur at Varysburg. At the top of the falls a layer of compact blue sandstone 5 feet thick is overlain by 4 feet of shales, that are succeeded by another layer of sandstone like the one below and 10 feet thick. The strata next above are covered, but black shale is exposed slightly a short distance up the stream. | These sandstones are in the horizon of the Portage sand- stones of the Genesee river section. They are near the surface over a large area in the town of Sheldon and outcrop in many places. They also outcrop frequently on the west side of the valley south of Johnsons Falls for 5 or 6 miles, to Java Village, where 8 feet of the upper bed are exposed on the upper side of the bridge over a small stream that comes in from the east through a deep ravine. _ The sandstone is here succeeded by 15 feet of black shale, next above which there are 145 feet of soft blue and olive Wis- coy shales with thin bands of black slates and a few thin flags. In the lower part of this section the rock is quite calcareous, and there are many concretions and concretionary layers. The upper part is more sandy. Buchiola speciosa and Palaeotrochus are common, and other Portage species occur in the lower soft shales. A layer of calcareous sandstone, 1 foot, 8 inches thick, forms the crest of a cascade 15 feet high and is 160 feet above the sand- stone at the mouth of the glen. It contains many small fragments of brachiopods,. very few of which are large enough for identification of species. This stratum is in every way like the fossiliferous layer at the top of the Tonawanda creek section, the outcrop of which is 5 miles east of this point, and it is without doubt the same. It is succeeded by 10 feet of softer, flaggy and shaly sand- stone and 35 feet of hard blue shales in which there are a few even flags. 1018 | NEW YORK STATE MUSEUM The only fossils found were a few brachiopods scattered through the shale and several impressions of Liorhynchus on the lower surface of a sandy layer. On the east side of the valley of Cazenovia creek, 114 miles north of Holland, the sandstones of the Portageville horizon are exposed in an old quarry and other places near the rail- road, and the black shales that succeed them may be seen in the bed of the stream in the village. | In a small ravine on the east side of the valley a little north of the railroad station, there is an exposure that begins about 50 feet above the sandstones, in which there occurs, 100 feet above the bottom, a layer of calcareous sandstone a foot or more thick, of the same character as the one in this horizon in the Java Village ravine, except that no fossils were found in it. A loose slab, fallen apparently from but a few feet higher, contained Liorhynchus, Ambocoelia umbonata and Orbiculoidea. Stations in the Tonawanda creek valley 25 Along the Tannery brook, 1 mile west of Attica. Exposed: upper Genesee, the Middlesex shales of the Portage and the Cashaqua shales. 26 Along Tonawanda creek and the railroad at Sierks station, 4 miles south of Attica. The top of the Rhinestreet shales and base of the Bristol shales. 27 Old quarry at the top of the hill on the west side, 114 miles south of Sierks. ‘The Gardeau beds and the base of the Portage sandstones. | 28 Ravine on west side at Varysburg. Gardeau beds and the Portage sandstones, | 29 The Stony brook ravine east of Varysburg. Gardeau beds. 30 Young’s quarry, and along the east branch of Tonawanda creek, 4 miles south of Johnsonburg. Fossiliferous sand- stone. eres RRR rs S REPORT OF THE STATH PALEONTOLOGIST 1902 1019 Stations between the Tonawanda valley and the shore of Lake Hrie 31 Along Murder creek at Griswold station. Exposed: upper Hamilton, Genesee shales, the Styliola limestone, the Middlesex shales, the Cashaqua shales and the Rhine- street shales. 32 Along Cayuga creek at Iron Bridge Mills. The Styliola limestone, Upper Genesee shales and the Middlesex shales of the Portage eroup. 33 Along Cayuga creek at Cowlesville. The Cashaqua shales. 34 Along Cayuga creek at Folsomdale. The Rhinestreet shales. 35 Along Big Buffalo creek at Porterville and East Elma. Rhinestreet shales and the Cashaqua shales. 36 Ravine at Johnsons Falls, 2 miles north of Strykersville. Gardeau to base of Portage sandstones. 37 Ravine at Java Village. Top of the Portage sandstones and the Wiscoy shales to Long Beards riffs sandstone. 38 Ravine east of, and along the railroad north of Holland. Portage sandstones and Wiscoy shales. 40 Ravine 1 mile south of West Falls. Gardeau beds. Lake Erie section The exposure of Portage strata on the shore of Lake Erie _ begins in the cliffs on the south side of the mouth of Eighteen Mile creek in the town of Evans, Erie co. and, through broken by many short stretches of sandy or gravelly beach, is almost continuous for 45 miles to the northwest corner of the town of Westfield, Chautauqua co. 8 miles from the Pennsylvania line. | , But three of the subdivisions that can be made in the Portage formation in the Genesee river section can be identified here by the character of the sedimentation. The Middlesex, the Cashaqua and the Rhinestreet shale are much alike in both sections except as to thickness, but above them there is in the lake section a thick mass of shales, light colored and more or less calcareous at places, black and bitu- 1020 NEW YORK STATE MUSEUM minous, in which flags or sandstones are absent from all the lower part, rare in the middle, and are a considerable portion Rhinestreet black shale Cashaqua shale f, i | it Middlesex black shale | | Styliola limestone Moscow shale Encrinal limestone Fic. 8 Cliff section oppo- site Hotel Mortimer, Lake Erie shore near North Evans. Station 50 of the sediment only at the very top of the section. Caleareous concretions and concre- tionary layers are of frequent occurrence. in all parts of the section. | . Fossils are common in the lower and the upper beds but are very rare in the middle ones. The fauna is composed al- most entirely of cephalopods, gastro- pods and lamellibranchs. Chonetes lepida occurs occasionally in the Cashaqua shales, a few Lingulas in the black slates and a small Productella near the top of the group were the only’ other brachiopods found. In the exposure in the south shore cliffs, 14 mile south of the mouth of - Eighteen Mile creek, the Styliola lime- stone is separated by 1 foot of dark shales from the top of the Hamilton shale. This limestone is 6 inches thick and inclined to be shaly, but is more compact and 12 inches thick where it comes down to the lake level 144 miles to the south. It is overlain by 11 feet of characteristic Upper Genesee shales, — that are succeeded by the black Middle- sex shale, which is here but 8 feet thick. The Cashaqua shales, also exposed in the cliff, are 32 feet thick, and consist of 24 feet of very light colored clayey shales, : and above these 8 feet of light and dark shales. Concretions are common throughout the formation. ; The upper part of the cliff is in the horizon of the Rhine- street shale, and the rock is all black slaty shale. 3 At the mouth of Pike creek 12 feet of IHlamilton shales, the Genesee shales and the Middlesex are exposed. REPORT OF THE STATE PALEONTOLOGIST 1902 1021 The base of the Portage formation is 12 feet above the lake ~ Jevel. Small Lingulas of two species occur in the black slates. The lower part of the Cashaqua shales is not exposed along Pike creek, but above the highway bridge, 60 rods from the lake, the upper part is well exposed in the bottom and sides of the channel. Fossils are common in the numerous concretions and some of the soft layers. The contact with the Rhinestreet shale is at the bottom of a low cascade, and: about 15 feet of the succeeding black slates are exposed in the sides of the ravine. In the ravine of Eighteen Mile creek the Middlesex shale is exposed in the cliffs in the vicinity of the two railroad bridges, and it is at the water level on the east side of the upper one. The lower part of the Cashaqua shales is covered in the bed of the stream, but the upper part appears in the escarpment on the east side 40 rods above the upper railroad bridge, and there is a large ex- posure of the same horizon in the ereek dark shales with large concretions black and blue shales black shale bed above the highway bridge at North eee Evans and for 50 or 60 rods eastward to the old dam. In the cliffs at the west end of the dam Gachanuin shale the contact with the Rhinestreet shale Fie. 9 Section on High- and 50 feet of the black shales may be _ teen Mile creek from North ¥ Evans totherailroad bridge seen. at Eden Valley. Station 51 Impressions of goniatites are very common in the Casha- qua shales, and in the concretions also a small Loxonema. Buchiola speciosa is very rare, but a few other lamelli- branchs appear frequently. The shale in the softer layers has about the consistency of dried clay and the only hard layers 1022 NEW YORK STATE MUSEUM are calcareous and concretionary. Spherical concretions are numerous, and some of them are 1 foot to & feet in diameter. The dugway roads leading down to the bridge at North Evans were excavated in the black Rhinestreet shale, and all of this formation is exposed in detail in the bottom and sides of the Eighteen Mile creek gorge between North Evans and the Erie Railroad bridge, 4 miles to the southeast. It is 185 feet thick in this section and is composed principally of bitu- minous black shale, but there are several layers of bluish shale, some of which are 6 feet to 8 feet thick, and in these lighter beds there are many large septaria and beautifully symmetric concretions. In two or three rows in the upper aise of the band the septaria reach a diameter of 6 feet to 10 feet and are 2 feet to 4 feet thick. The lighter layers contain a few fossils like those found in the Cashaqua beds. The black slates are almost barren, except of plant remains, which are quite common. In the cliff at North Evans a small Lingula occurs in one of the lower black layers. These shales are exposed at several places along the lake shore on the north side of Sturgeon point and along the railroads in the vicinity of Derby. A concretionary layer 6 inches to 8 inches thick, the upper surface of which is a scraggly mass of angular fragments of — impure limestone, separated by thin seams of spar, like the sur- face of a flat septarium but finer, is taken as the top of the Rhinestreet shale, the proportion of black shale above this hori- zon being less than the lighter. It is exposed under the Erie Railroad bridge over Eighteen Mile creek below Eden Valley and near Angola, and on the lake shore. The lighter shales that succeed the Rhinestreet shale are ex- posed in a small ravine that comes into the gorge of Eighteen Mile creek from the east about 60 rods above the Erie Railroad bridge. The section covers about 100 feet, in which there are many large and small spherical concretions and others that are oblong and flattened. Very few of them are septaria. This horizon is stratigraphically continuous with the Hatch Shales and flags of eastern sections, but its lithologic characters have changed somewhat. REPORT OF THE STATE PALEONTOLOGIST 1902 1023 The same horizon is exposed in the cliff on the west side of the main ravine and in the creek bed below the highway bridge 14 mile farther south. The scraggy layer at the top of the Rhinestreet shale outcrops at the lake level at Fox’s point on the south side of Dibble bay 214 nodular shale light blue and olive shale with thin black an concretionary layers light soft , shales with large flat concretions light shales wit } concretions light and dark shales wit concretions _Fie. 10 Section on Big Sister creek from Evans Cen- ter to Pontiac. Station 52 miles west of Angola, and about 60 feet of the light shales next above it and several rows of the large concretions are exposed in the escarpments along the shore for a mile to the mouth of Mud creek. The rock exposure on Big Sister creek begins about a mile from the lake shore. About 50 feet of the Rhinestreet shale may be seen in the bottom and sides of the creek in the vicinity of Evans and southeastward to the escarpment on the north side of the Angola cemetery. At the foot of the south end of this low cliff the concretionary layer crosses the chan- nel, and it can be traced in the cliff, rising rapidly toward the north. Between this layer and a soft cal- careous sandstone 4 inches thick, con- taining many nodules of iron pyrites that is exposed in the cliff on the north side of the creek 20 rods above the Lake Shore Railroad bridge at Angola, there are 68 feet of light soft shales, in which there are a few thin, black layers and several rows of flattened concretions, from 2 feet to 4 feet long and 8 inches to 12 inches thick, besides many smaller ones. Manticoceras rhynchostoma and other cephalopods occur, finely preserved in the concretions and the shales contain a few lamellibranchs. - This horizon is the same as that at the top of the previously described section on Eighteen Mile creek. It is also exposed 1024 NEW YORK STATE MUSEUM aleng Delaware creek a mile west of Angola and in the escarp- ments on the lake shore, north of the mouth of Mud (or Farn- ham) creek. | Between the 4 inch sandstone in the escarpment at Angola previously referred to, and the top of the rock exposure at Pontiac there are exposed in the ravine of Big Sister creek about 100 feet of soft, light colored shales in which there are a few black layers, but no flags or sandstones. Altogether the beds are much like the Cashaqua beds, except that concretions are much less frequent, and most of them are quite small, but there are many concretionary layers from 2 inches to 4 inches thick. sabes | These beds are also abundantly exposed in the quarries of the Buffalo Sewer Pipe Co., 4% mile south of Angola, and along the Lake Shore Railroad in the rock cut between the Delaware creek culvert and Farnham. A few low escarpments along the lake shore between. the mouths of Mud creek and Cattaraugus creek are in the hori- zon of the upper part of the section on Big Sister creek. At Pontiac there are two thin beds of light shale in which there are embedded great numbers of smail calcareous nodules or concretions that give the beds a pebbly structure. They are | separated by 4 feet of light shales, in which the pebbles do not appear. A layer of black slate 2 feet thick is 4 feet above the upper pebbly layer. This horizon is exposed in the cliffs on the south side o Cattaraugus creek and a few feet above the water on the south side of the mouth of Silver creek. The black layer appears in the bottom and sides of Walnut creek, near the Emke flouring mill in the south part of the village of Silver Creek. There is an almost continuous exposure of upper Portage and lower Chemung strata along the channel of Walnut creek for more than 10 miles south from pea Creek, the first 8 miles in a deep gorge. In this ravine next above the 2 foot black layer near the mill, there are 112 feet. of shales, nearly all light colored except two dark beds each 11 feet thick. The bottom of the first is 15 REPORT OF THE STATE PALEONTOLOGIST 1902 1025 feet and the second 56 feet above the base of this section. These beds are equivalent to the upper part of Hatch flags and shales of eastern sections. Dunkirk shale. A third black band, the Dunkirk shale, similar in character to the Middlesex and the Rhinestreet shales, succeeds the 112 feet of lighter beds and is 55 feet thick. At the bottom there are 35 feet of densely black, slaty shales, like those in the other black bands and containing the shales and flags same species of Lingula. The base of this shale is exposed in the cliffs on the south side of Dunkirk harbor and in the escarpments on the west side of Point Gratiot. The septaria are strewn along the beach 2 miles southwest in the vicinity of Van Buren point. The same beds are exposed in the bot- tom and sides of Silver creek under the high bridge at Hanover Center and in two large ravines near North Collins, and along the highway on the hill 1 mile east of Eden Center in Erie county. ‘Above the Dunkirk shale light, soft shales again predominate, but layers of black shale light shale black shale light shale black shale from an inch to several feet in thickness occur very frequently, and con- cretions are common. A row of very large septaria 148 feet above the black band in the Walnut creek Section appears on the lake shore opposite Hick ld: SectnsoReaWal- Brocton. A sandstone 4 inches thick lies villus noe 7 Cones. just above the septaria and flags, and thin Se aes Sandstones increase in numbers and thickness above this hori- zon. They are very rare below it. A band of soft shales 67 feet thick, in which there are a few flags but concretions are almost entirely absent, is succeeded by a band of similar shales and flags 25 feet thick in which there are several rows of concretions. dark and light shale 1026 NEW YORK STATE MUSEUM Fossils are common in a few of the layers of shale, and, in two rows of large flattened concretions, that are not septaria, there are some finely preserved cephalopods and large lamellibranchs. All these beds are stratigraphically equivalent to the Gardeau of eastern sections, more particularly its upper part, and prob- Laona . sandstone blue shales and thin sandstones flags and shale dark shale with coneretions light and dark shale i dark slaty shales Fic.12 Section onWalnut ereek from Keech’s Corners to sandstone at Corey’s mill, ‘Forestville. The upper part from the succession in Terry’s ravine. Stations 60, 61 ably in some degree to the Portage sand- stone horizon. This horizon is exposed along Walnut creek below and above the Erie Railroad bridge at Forestville and in a small ravine 14 mile west of Smith’s Mills. It is bare at the water level on the lake shore at Correll’s point, one the vil- lage of Portland. Next above the upper row of large con- cretions in the Walnut creek ravine at Forestville, there are 40 feet of soft, light and dark shales in which there are many small concretions and that are succeeded by a flaggy band 10 feet thick, that pro- duces a cascade about 20 feet high by the ‘mill on the north side of Main street. Another band of light and dark shales with a few thin flags and small concre- tions, that is about 50 feet thick, overlies the flaggy band and is succeeded by a bed of sandstones and flags separated by thin layers of hard blue shales, that is 22 feet thick, the base of which is the top of the Portage formation on Lake Erie. The Laona sandstone (Hall) is an arena-_ ceous stratum well exposed at the falls in Terry’s ravine, 1 mile northeast of Forestville, where brachiopods (Spiri- fer disjunctus etc.) occur abun- - dantly in some of the light colored layers of sandstone, in place. in the lower part of the stratum and in several large fallen slabs in the ravine below the falls. REPORT OF THE STATE PALEONTOLOGIST 1902 1027 It is also exposed in Faulkner’s gulch, a ravine about 5 miles east of Terry’s ravine on the road from Smith’s Mills to Nash- ville, and a compact layer in the lower part contains brachiopods in still greater numbers, both of individuals and of species. Some loose slabs in the gorge of Walnut creek, below the mill at Forestville, from this horizon also, contains brachiopods, but they were not found in place in the Walnut creek section. The sandstones cause a cascade at Corey’s mill, 34 mile south of Forestville, and a layer about 50 feet higher, exposed in a small ravine a mile farther south, contains several species of brachiopods, and they also occur along the escarpment on the east side of the creek at Miller’s Mills, a mile farther south. A layer 4 inches thick, and quite calcareous, that is exposed in the bed of a small brook that flows through Forestville from the east, contains several species of brachiopods. The horizon is about 75 feet above the sandstones. There are several quar- ries and natural outcrops between Forestville and Laona in which the sandstones are exposed. At Laona they appear in the bed and sides of Canadaway creek, and one compact layer 5 feet thick has been quarried for more than 50 years. In a soft layer in the bed of the stream about a mile south of Laona and 75 feet above the sandstones a few obscure im- _ pressions of indeterminable cephalopods were found. No other representatives of the Portage fauna were found above the horizon of the Laona sandstone, in the Lake Erie section. On the lower surface of a thin sandstone, 10 feet higher, and in the subjacent shales, Chemung brachiopods are common. Shumla sandstone (Hall). The sandstones exposed at Shumla 214 miles south of Laona are 260 feet to 280 feet above the Laona sandstone. Fossils are very rare here, but a few speci- mens of a small Orthis and a small Productella are distributed through the beds and are quite common in the large concretions in a thick sandstone in the bed of the creek under the bridge. The position of the Laona sandstone may be easily traced toward the southwest by the means of a number of small out- crops. It is exposed at Brocton in the bed of Slipperyrock creek near the bridge in the northwest part of the village and 1028 NEW YORK STATE MUSEUM in a field quarry 50 rods north; also in a small quarry 5 miles southwest from Brocton near the lake road, in the sides of a Laona sandstone - Portland gray shales with concretions and few flags Dunkirk black shale =| Silver Creek light soft shales | | it ] | Angola soft == =| shales with” concretions | Rhinestreet black shale Cashaqua shale Middlesex shale Genesee shale Fie. 13 Section on Lake Erie from top of Hamilton to top of Laona sandstone. Stations 50- small ravine and in a quarry similarly situated 1 mile farther southwest. The sandstones in this horizon are _ constantly thinner bedded and_ less compact in the exposures. southwest from Forestville, and they appear in the upper part of the cliffs on the lake shore northeast from Barcelona (Port- land Harbor) as a band of flags and thin sandstones and disappear under the waters of Lake Erie about a mile southwest from the mouth of Chautau- qua creek and 9 miles northeast from the Pennsylvania line. The sandstones of the Shumla horizon are exposed in the sides of Chautauqua creek ravine in the village of Westfield near the milldam, and in the cliffs along the lake shore from 144 to 3 miles north of the state line, and they come down to the lake level under the gravelly beach 44 mile north of the state line. Fossils of any description are exceed- ingly rare in the shales and flags be- tween the horizons of the Laona and the Shumla sandstones along the lake shore, the only ones found being a few small brachiopods in the intermediate beds on Chautauqua creek and in about the same horizon in the bed of a small creek that flows into the lake near a fishing station 4 miles southwest from Westfield. | At Northeast Pa. Chemung brachiopods were found in small calcareous masses on the uneven upper side of a 4 inch flag and on the lower surface of a similar flag 5 feet higher, both of which are exposed in the bed of Twelve Mile creek, 14 mile from the lake and about 30 feet above it. REPORT OF THE STATE PALEONTOLOGIST 1902 1029 In the 500 or 600 feet of shales and flags exposed along the bed of this stream above the horizon in which the brachiopods occur, and below the highly fossiliferous Chemung sandstones 3 miles east, plant remains are common, but other fossils have not been observed. 50 ol 52 62 64 Stations on or near the shore of Lake Erie The shore of Lake Erie from the mouth of Eighteen Mile creek to the mouth of Pike creek. Exposed: upper Ham- ilton shales, the Genesee shales, the Middlesex shales of the Portage group and the Cashaqua shales. The ravine of Eighteen Mile creek, from North Evans to Eden Valley. The Cashaqua shales and the Rhinestreet shales. Along Big Sister creek from Evans to Angola and Pontiac. The Rhinestreet shales and the Bristol shales (or Angola shales). Along the lake shore from Fox’s point to the mouth of Mud ereek. Bristol shales. : Along the lake shore from Irving to Dunkirk. Silver Creek shales. Walnut creek ravine from Silver Creek to Keech’s Cor- ners. Silver Creek shales and Point Gratiot shales. The lake shore from the mouth of the Little Canadaway ereek to the mouth of Slipperyrock creek, opposite Brocton. Portland shales. Lake Shore at Correll’s point. Portland shales. Along Silver creek at the High bridge and Smith’s Mills, and ravine 1 mile west of Smith’s Mills. Portland shales. Along Walnut creek at Forestville. Portland shales. Terry’s ravine, 1 mile north of Forestville. Portland shales and the Laona sandstones. Lake shore in western part of the town of Westfield. The Laona sandstones. Along Canadaway creek at Laona. The Laona sandstones. Along Twelve Mile creek 14 mile from the lake shore at Northeast Pa. Thin sandstones containing brachiopods. STRATIGRAPHY OF BECRAFT MOUNTAIN!, COLUMBIA COUNTY, N. Y. | With stratigraphic map and sections BY AMADEUS W. GRABAU Introductory . Becraft mountain, close to the city of Hudson, has been known to geologists since the early days of geologic study in the State of New York, and descriptions of it play an important part in the early reports on the geology of the State. Ina letter dated — Dec. 3, 1820, and published in Silliman’s Journal for 18222, Mr John P. Jenkins, of Hudson N. Y., gave a brief description of Becraft mountain. He calls it“. . . a solid mass of gray rock supporting a blue compact limestone; the upper strata of both rocks contain a great variety of petrifactions which have been described by Mr Eaton and others.” In 1823 Silliman described the “marble of Hudson,” which was wrought by Mr Charles Darling of that city. He considers it of high class, and similar to that of the Peak of Derbyshire. — The “marble” is the Becraft limestone of Becraft mountain. Mather® in 1838 gives a description of the strata of Mount Becraft and of Mt Bob, which lies a little to the north, as well as their general structure, and states that the limestone of the mountains lies unconformably on the Hudson river slates. In 18404 he compared the strata of the Helderberg mountains with those of Becraft, considering them similar. In 1841° he again refers to Becraft, emphasizing the unconformity between the “nearly horizontal” Helderberg limestones, and the “highly inclined” subjacent Hudson river strata. In his final report, 1843°, Mather describes Becraft mountain, © and gives three sections to illustrate the structure. The descrip- highest elevation on it is less than 500 feet above the sea. Structurally, how- ever, it is a section of a mountain range. All the localities may readily be vis- ited in a short walk from Hudson N. Y., where good accommodations may be - obtained.at the Worth house, or in private boarding houses. 2 Am. Jour. Sci. 1822. 4:33. 8 Geol. N. Y. lst Dist. 2d An. Rep’t. 1838. p.165, 166. ‘Geol. N. Y. lst Dist. 4th An. Rep’t. 1840. p.238. *Geol. N. Y. Ist Dist. 5th An. Rep’t. 1841 p90. — °Geol. N. Y. 1st Dist. Final Rep’t. 1848. p.344-52, pl. 24, fig. 4-6. REPORT OF THE STATE PALEONTOLOGIST 1902 1031 tion is largely a repetition of that of 1838. He recognizes three formations overlying the Hudson river beds, viz (1) the Water- lime group, including the Tentaculite limestone (Manlius), (2) the Catskill shaly limestone (New Scotland), and (3) the upper, Scutella, or Sparry limestone (Becraft). The Coeymans and Kingston were not differentiated from the limestones respec- tively underlying each, and the higher strata were not recog- nized. He determined the essential basin-shaped structure of the mountain, and the unconformity between the lowest bed of the series, and the underlying tilted and eroded Hudson river strata. This unconformity is depicted in his section 6, which furthermore illustrates with section 4, what he believed to be a series of tilted fault blocks. This structure was undoubtedly suggested by the numerous cuestalets which characterize the outcrops of the New Scotland, and to some extent the other beds also. The steep infaces or fronts of these erosion ridges and the surface slopes of their tops, which follow the dip, have all the aspect of the corresponding faces of slightly tilted fault blocks [fig. 1, a, b]. Mather also gives a section of the south- east end of Becraft mountain, which shows the overturned strata on the east. err yey SS Fig. 1 Diagram illustrating the detailed structure of parts of Becraft mountain: a, as in- terpreted by Mather; 5b, as actually existing. In 1846 Emmons! gave a section of the southeastern end of Becraft mountain, showing a conformable relation between the Hudson river and overlying waterlime. He also speaks of a mass of Calciferous sandstone supported by the Taconic slate. This refers probably to the hill of Burden conglomerate opposite the center of the eastern face of the mountain. In 1858 Rogers? mentions the unconformity at Becraft, which he states he discovered in 1837. He says: ~The lower Helderberg or Pre-meridian rocks are seen in hori- zontal stratification in the hill, while the Hudson river slates —— —— — — — — —— — — — —————————— —————————————— — — —— —————— ————————— - -! Agriculture of New York. 1846. 1:136. _* Geology of Pennsylvania. 1858. 2:785. 1032 NEW YORK STATE MUSEUM around its base are steeply inclined, and contorted from a move- ment previous to the deposition of the shales and limestones upon them. Hall in 18591 expressed a doubt as to the reported uncon- formity between the Hudson river and Lower Helderberg strata, since “in Becraft’s mountain the strata of this age [Lower | Helderberg and Waterlime] lie inclined above the Hudson river group, and there appears no positive evidence of their uncon- formability.” | The most complete review of the literature of Mt Becraft and the neighboring region on both sides of the Hudson is given by Davis in his article on the folded Helderberg limestones east of the Catskills.27 From a study of this region on the west bank of the Hudson, he concludes that the contact between the Hud- son river shale and the Waterlime is a conformable one, though he considers this conformity difficult to understand in view of the variation of the strata. . | In 1883? Davis published the first eeologic map of Becraft mountain and gave the first comprehensive account of its strati- graphy and structure. The map is accompanied by a number of cross sections, which give the main structural features of the range. He. recognizes the Waterlime (Manlius) resting on the Hudson river beds and discusses at length the evidence for and against the unconformity between the two. While leaning toward the acceptance of an unconformity, he nevertheless considers the evidence for it still insufficient. Above the Waterlime he recog- nizes the Lower Pentamerus (Coeymans), the Delthyris shaly (New Scotland), the Upper Pentamerus (Becraft), the Cauda- galli (Esopus) and the Corniferous (Onondaga). He did not differentiate the Kingston (Port Ewen) and Oriskany from the Becraft, nor the Schoharie from the Esopus. He also recognizes the complicated southeastern portion of the mountain. Clarke* has published the latest and most complete map of — Becraft mountain extant. In this all the formations are de- , Palaeontology of New York. 1859. 3:39. ? Mus. Comp. Zool. Bul. v.7 (Geol. Ser. v.1) p.311-30, pl.12-13 * Am. Jour. Sci. ser. 3. 1883. 26:381-89. * Clarke, J. M. Oriskany Fauna of Becraft Mountain, Columbia County, N. Y. N. Y. State Mus. Mem. 3. 1900, REPOR' OF THE STATE PALEONTOLOGIST 1902 1033 picted in their proper relation, he having added to those recog- nized by Davis, the Schoharie, the Port Ewen and the Oriskany, the latter formation having been discovered by Beecher and Smock at Becraft in 1890.1 No attempt was made by Clarke to depict the minute details of the distribution of the formations, nor to map the compli- cated structure. The latter could be worked out only by a minute following of the outcrops over the entire field, and by a careful determination of the beds in isolated outcrops. For the latter work, paleontologic data had to be relied on fully as much as lithic characters, since the latter are often nearly identical in distinet horizons. The desirability of a carefully constructed map of Becraft mountain has long been felt, not only on account of the inter- esting stratigraphic as well as tectonic features, which throw light on the problem of Appalachian stratigraphy and struc- ture, but also on account of the fact that Becraft mountain forms an ideal region for field work with students in geology. Being isolated from the rest of the Helderbergs and of conveni- ently small size, it presents a problem of proper circumscrip- tion to enable something like completion to be attained by the students in the field. Its range of strata, with their well pre- served fossils, most of which are limited to few or only one of the horizons; the various complications by folds and faults of several ages, together with all the more prominent tectonic features accompanying them, and the interesting stream ad- justments and other physiographic features, make this an almost unrivaled field for classwork. Recognizing this fact, Dr John ©. Smock, of Hudson, had constructed a detailed topographic map of the region, on the scale of 6 inches to the mile, and with contour intervals of 10 feet. This map has served as the basis of the accompanying geologic map, which was prepared under the auspices of Prof. John M. Clarke, the state paleontologist, and with the partial cooperation of stu- New York, with an annotated list of fossils by J. M. Clarke. Am. Jour. Sci. 1897. 44:410-14 7 1034 NEW YORK STATE MUSEUM . dents in the Summer School of Geology in Columbia University. Nearly all the collections of fossils which have served as the basis of the accompanying faunal lists, were made by the uni- versity parties under the direction of the instructors. The col- lection, however, on which the list of Port Ewen fossils is based | was made by myself, that I might be certain of the range of the species. A general map was prepared by the field parties, which afterward served me as a further basis for detailed study. I wish here to express my indebtedness to Prof. J ohn C: Smock, who not only furnished us with the accurate topographic base map, but also rendered other assistance during the progress of the field work. STRATA OF THE BECRAFT REGION The following formations are exposed at Becraft mountain. The thicknesses appended are the best estimates, whenever actual measurement was not possible. | Feet 11, Onondaga limestones: --A5- ee ae 20-25 10; Schoharie eriten . 5 4. sce oe oe 200 9 Hsopus 2rit... ta. Mae Aes eae ne an 100 Deeauia 8. Oriskany Quartzite.) aso deeds abe > lees 7 Port Ewen (Kingston) limestone............ ee 6 Beéraft. limestone. 22 4b tgs ata ee 40-45 5 New Scotland shaly limestone.............. 70-75 4. Coeymans, limest@ne fej. a ciaacgyt ect bee 42-45 Siluric 3 Mantiine limestone... 6 51.08 eto bade eee oe 55 Cham- 2 Hudson river slates............ ren Vaan ae plainiec 1 Burdensconslomerate: . 2.) ices halieiiier- peeree 1 BURDEN CONGLOMERATE This name is proposed for a calcareous conglomerate in which > the pebbles are chiefly limestone embedded in a silicious sand, which in turn is held together by a more or less calcareous _ cement. The limestone of the pebbles is in part a gray, compact rock (calcilutite!) not unlike the Manlius limestone and in part a more granular mass (calcarenite (Grabau)). The matrix is 1Grabau. Science Feb. 20, 1903. p.297. Also Geol. Soc. Am. Bul. v. 14; Paleozoic Coral Reefs, with notes on the classification of limestones. é REPORT OF THE STATE PALEONTOLOGIST 1902 1035 generally stained with iron hydrate, and at the Burden iron mine this rock is in intimate association with the iron ore. Davis described this rock,! assigning to it an age “ apparently younger than the Helderberg series, and certainly much older than the drift.” He thought that the limestone fragments - “seem to correspond with the several subdivisions of the Lower _ Helderberg.” He found it at two localities, one in the meadow south of Academy hill and one in the fields a quarter of a mile south of the southern end of the mountain. It is well exposed on a little stream which enters Claverack creek at a point about east of that where fault 16 strikes the eastern bounding road of the mountain. The stream lies on a fault line. It. has cut back some distance from Claverack creek and forms a fall over the hard conglomerate, which fall has been utilized as a site for a dam and mill. The conglomerate bed is about 10 feet thick at the fault. It dips northeastward and abuts against what are probably the Normans kill shales, which have a similar dip. The conglomerate increases in thickness away from the fault and forms a prominent hill between the road and the stream. It is underlain by shales similar -to those ll 1y{\l i i on the opposite side of —= the fault [fig. 2]. ——— The age of this con- === gt eee glomerate is unknown. SS I, Z That it belongs to the = a ee em Hudson river series is un- 23 = == SS SS doubted, but whether Fig. 2 Fault between Burden conglomerate (a) older or younger than and Normanskill shales (6) the Normans kill shales, has not been ascertained. No fos- sils have been noted in the pebbles of limestone, though some search has been made for them. The position and char- acter of the bed indicate that the rock is older than the beds composing Becraft mountain, for all these beds with the ex- ception of the Manlius are highly fossiliferous and easily Am. Jour. Sci.’ 1883. 26:382. ~ LUG NEW YORK STATE MUSEUM recognizable. It may correspond to the Trenton conglomerate of Rysedorph hill described by Ruedemann,! or it may be of still earlier date. Its areal relations seem to indicate that it is older than the Normans kill beds of Mt Moreno. Boulders of this rock have been found on Becraft mountain in such a loca- tion that they could not well have been derived f10om any known outcrop. They therefore suggest other outcrops to the north — or northeast of Becraft mountain. 2 “HUDSON RIVER”? SHALES uF) Ruedemann has shown that the Hudson river shales do not constitute a single stratigraphic unit but rather comprise all the formations from the Beekmantown up to the top of the — Lorraine. Nevertheless, these shales constitute a formational unit, with but slight lithic variations, representing continuous deposition, and hence it is advisable to retain the local name, Hudson river group or shales, for this series. At Mt Moreno these shales contain a typical Normans kill fauna in the higher beds. Clarke cites Coenograptus gracilis, Didy- mograptus sagittarius, D. tenuis Hall and other species of graptolites.2. In the lower beds Phyllograptus was found by the Columbia field party. A recent visit in company with Dr Ruedemann resulted in the rediscovery of the Phyllo- eraptus beds in the lower layers at the northwest end of Mt Moreno. In these Dr Reudemann identified Phyllograptus angustifolius Hall, Trigonograptus ensiformis Hall, Climacograptus pungens Rued. (ms), Diplo- graptus dentatus Brogn. and Phyllograptus pos- tremus Rued. (ms). Dr Ruedemann refers these beds to his third Deep kill zone or zone with Diplograptus denta- tus which may represent a Beekmantown horizon. Though no fossils have been obtained from the Hudson river shales of Becraft mountain, it is probable that they are of the same, or perhaps somewhat earlier. age. Some of the strata underlying the mountain are somewhat more compact and firmer textured ?Ruedemann. Trenton Conglomerate of Rysedorph Hill. N. Y. State Mus. Bul. 49. 1901. p.3. Oriskany Fauna of Becraft Mountain. 1900. p.7, footnote. REPORT OF THE STATE PALEONTOLOGIST 1902 1037 than those of Mt Moreno, as noted by Davis. Beds of hard sili- cious limestone are also found intercalated among the other strata. Similar beds are met with on Mt Moreno. Contact between the “Hudson river series” and the Manlius formation. This contact is everywhere a markedly unconform- able one, the Hudson river strata being much folded and trun- cated by erosion before the deposition of the Manlius limestone. The unconformity takes the place of the strata from the Medina to the Waterlime of Buffalo inclusive, which apparently were never deposited in this spot. The later Champlainic strata, including the Lorraine, Utica and probably part of the Upper Trenton, and perhaps also the Oneida conglomerate, were worn away during the period of deposition of the Siluric strata west of the Hudson. The actual contaet between the Champlainic and Siluric strata is shown only in a few places at Becraft. The most important of these is at the outlet of the spring supplying the Hudson aqueduct. This is at the extreme northern point of the mountain. The dip cf the Hudson river strata here has not been ascertained, but the cleavage planes stand vertical. The Man- lius rests directly on the Hudson river strata. Another expos- ure of the contact is on the old tramroad leading to the ~quarries, a little north of the Jonesburg road. The strike of the Hudson river beds is here n. 50° e. and the dip is 35° s.e., the rocks being thin bedded and fissile. The Manlius is seen in the upper part of the cliff, but much disturbed by frost action and slipping, so that the precise character of the contact can not be determined. The dip of the Manlius a little higher up the cliff is from 10° to 12° eastward. A few exposures of the Hudson river beds in the Ancram road south of this, allow the approximate continuation of the contact line. The most continuous exposures of the Hudson river—Manlius - contact are found on either side of Fred. G. Lambert’s farm, in the hills facing faults 20 and 21 [see map]. Here 80 feet or more of the Hudson river shales are exposed and the contact can be traced on both sides for several hundred feet, though generaliy the actual line of contact is covered. The Hudson 1038 NEW YORK STATE MUSEUM river beds are much disturbed. Between faults 18 and 17 ex- posures of both rocks allow the tracing of the contact line with fair accuracy, but beyond that the contact can be only approxi- mately determined, since the exposures of ths Hudson river beds are found only at intervals and then at some distance from the Manlius exposures. | That there actually is an unconformity between the two sets of strata hardly admits longer of a doubt. Besides the clear indication of the disturbance of the Hudson river strata and the erosion of their upper surfaces, the great time hiatus, extend- ing from the middle Lower Siluric to near the top of the Upper Siluric, is sufficient indication of an unconformity and would Fig. 3 Contact of Manlius limestone (6), with Hudson river shales (a) and Coeymans limestone (c), northern margin of Becraft mountain be, even if this were not brought out in the structure. Such an absence of formations, when not due to’ faulting, as is clearly not the case here, can be accounted for only by nondeposition or by subsequent erosion. And the former in this region at least is, like the latter, indicative of land conditions. | REPORT OF THE STATE PALEONTOLOGIST 1902 1039 3 MANLIUS LIMESTONE The best place for the examination of the Manlius limestone of Becraft mountain is along the northern margin of the moun- tain, in the city quarry, and at the Hudson aqueduct. At the latter place, just west of the old tavern in Greenport, the entire thickness is shown. At this point a powerful spring issues from the mountains, the water of which supplies the pumps in the city of Hudson. In the bed of the stream formed by this spring the “ Hudson river” slates are exposed. They are much contorted and cleaved, the cleavage planes standing vertical. The direction of bedding could not be determined. Resting on this are the lower Manlius beds, with a dip of 35° to 40° south- ward, the strike being n. 70° e. A little higher up the dip flat- tens to 20°, which is normal for the rock at this point. The measurements at this point are as follows [see fig. 3]: From basal contact to base of vertical cliff, the interval si being a slope with the rock more or less concealed..... 18 Hight of cliff portion 34 feet, which, with dip of 20° gives meereme thickness Of the beds....5.........c00ec eee cee 32 Thickness of beds forming upper slope from edge of cliff _ to contact with overlying Coeymans................. 5 Wort ehickness of Manlius. 200 eee ee: 5D No fossils were found at this place. At the city quarry in the cemetery off the Newman road (middle longitudinal mountain road) a total of 28 feet of the Upper Manlius is exposed, only 18 feet of which however are shown in the northeastern end of the quarry wall. It is over- lain by 32 feet of Coeymans limestone. (Fig. 4) The limestone in this as in the other exposures is a compact finely stratified lime-mud rock, a type of deposit for which the name calcilutite has recently been proposed! Leperditia alta is fairly abundant in certain layers in the upper part of the series, and is the only fossil found in these beds outside of the Stromatopora layers noted below. The dip of the strata is 12° s.e., the strike is n. 40° e. 3 1Science. n.ser. Feb. 20, 1903. p. 297. 1040 NEW YORK STATE MUSEUM Just below the lowest bed of the Coeymans limestone occurs the upper Stromatopora bed, forming the topmost layer of the Manlius. It averages 314 feet in thickness, varying between 3 and 4 feet, and is for the most part made up of masses of stromatoporoids piled one above the “other. ) In weathered ‘sec tions these masses are well shown, being less readily seen in the fresh section on account of the massiveness of the rock. Sometimes at the edge of the cliff they are weathered out, so that they look like piles of boul- ders. The largest head measured is about 114 feet in diameter. The bed immediately above this layer contains Favosites, crinoid joints and Gypidula galeata, and in texture-is finely crystalline. This crystal- line matrix frequently extends Me # Cts qo) oe ees down between the Stromatop- “?omatcvonmbed:) So) aa ora heads, but more frequently the fine mud-rock fills the inter- stices between the masses of hydrocoralline. The lower line of the Stromatopora. bed is very irregular, and sometimes a Stroma- topora is embedded in the stratified Manlius below. The “Stromatopora” fragments probably all belong to the genus Syringostroma of Nicholson, but their exact determina- tion is a matter of great difficulty on account of their unsatis- factory preservation and it has not been attempted. * Besides the stromatoporoids, the following fossils character- ize this bed. ihe Spirifer vanuxemi Hall This species is represented by a few individuals in the upper -Stromatopora bed. They agree substantially with the figure of Orthis plicata given by Vanuxem, which is the ehar- — acteristic Manlius limestone species of eastern New York. The median sinus of the pedicle valve of our specimens is shallow, REPORT OF THE STATE PALEONTOLOGIST 1902 | 1041 rounded at the bottom, and somewhat narrower than is usual in this species. It is flanked by about four rounded plications . on each side, which widen gradually toward the front of the shell. The brachial valve has four plications on each side of the central Ui i fold, the fourth being very short and ky” much fainter than the others. The Fig. 5 Spirifer vanuxemi, Median depression along the top of S eapheile the fold is marked in some cases, in others it does not occur at all. The plications, as well as the sinus and fold, extend to the apex. So far as I have been able to examine specimens of S. vanuxemi typical of the Manlius of eastern New York, the de- pression in the’ median fold of the brachial valve, where it occurs, is a feature of maturity rather than characteristic of the entire shell. In a few cases the depression in the fold can be traced nearly or perhaps quite to the apex of the valve. When the depression is well marked, the plications appear sharper and comparatively narrower. They also extend farther up the beak. On the other hand, it appears to be the case that, when the depression in the fold is faint or absent, the plications are less defined and near the apex become obsolete. Neverthe- less, there are individuals in which the depression in the fold and the broadly rounded plication occur together. Finally, individuals occur (as figured by Hall) in which the apical por- tion is free from plications, these beginning part way down. In this case they are, so far as observed, broad and rounded. The young individuals of the species are in all cases marked by less pronounced and fewer plications. In certain forms, which may be considered the more primitive representatives of the species, the young are practically free from plications, or if these occur, they are broadly rounded and low, one or two only occurring on each side of the fold or sinus. From these considerations we arrive at the conclusion that the ancestral type from which S. vanuxemi was derived, was a pauciplicate if not nonplicate form. Furthermore, that those individuals among the species which have few and low plications, with a 1042 NEW YORK STATE MUSEUM smooth apical portion, are the least accelerated, while the extreme of acceleration would show strong plications on the beak, with a median depression on the fold, which in extreme cases commences near the apex. In rare cases is there a faint median fold in the sinus of the pedicle valve. Similar modifica- tion through greater or less acceleration is found in the mid- . Siluric relative of this species, S. crispus, which seems to be a parallel development. hae | Spirifer corallinensis Grabau | Geol. Soc. Am. Bul. 1899. 11:352. This name was proposed, as a varietal one, for the character- istic Spirifer of the Coralline (Cobleskill) limestone of Scho- harie. This was referred by Hall toS.crispus and figured on plate 74, Paleontology of New York, v.2. The type speciment is transverse, wider than high, with rounded ends. The sinus of the pedicle valve is very shallow, rounded and. - narrow. Beak of pedicle valve incurved and area comparatively low. In this respect the species is like S. crispus. In a weathered-out specimen Fie. 6 Spirifer rallinen- surface markings similar to S. cris pus are shown. %1%Pedicle valve This species approaches closest to the simpler types of the New York S. crispus, that with fewest plications. A speci- men from Lockport [Am. Mus. col.+7%7+ | shows the relatively high and subrhomboidal outline, with a shallower sinus, which is rounded and widens less rapidly than in the normal form of S. crispus. There is one moderately strong and one very faint rounded plication on each side of the sinus, and two similar though fainter plications on each side of the fold. Dimensions of the type specimen, length 11.5 mm, hight of pedicle valve 10 mm, of brachial valve 8 mm, transverse diameter 7 mm. Another characteristic specimen from the - same bed (Coralline of Schoharie) is figured by Hall [fig. 8d]. It is proportionally narrower than specimen fig. 9d—-f, and has a somewhat more pronounced almost subangular sinus. The — width of this specimen is 11 mm, hight of pedicle valve 10.5 mm. ' Op. cit. pl. 74, fig. 9 d-f. Am. Mus. col. no. 447+. \ REPORT OF THE STATE PALEONTOLOGIST 1902 1043 Still another characteristic pedicle valve from the same horizon has a width of 18 mm with a hight of 16 mm, but is very ventri- cose, appearing proportionally higher. The plications are almost invisible and the sinus narrow, very shallow and rounded. This species is well represented in the upper Stromatopora bed of the Manlius limestone in the city quarry at Becraft. Its main distinguishing features are its subrhomboidal outline, shallow, narrow and rounded sinus, and obsolete or faint, broadly rounded plications. In the latter two features it differs materially from S.eriensis Grabau. Measurements of two characteristic pedicle valves from this bed give 1 2 PerenO MI MIE. Stik ae it sey oe rake 12 “DE UD EAT S60 (0 ae eee oer earner anne rae 9 10 A comparison of typical S. coralliensis with the types of S. modestus from Cumberland Md. shows a close rela- tionship, the latter differing chiefly in its extremely shallow sinus and faint fold, and in the total absence of plications. Specimens similar in most respects to typical S. corallin- ensis have been found in the Cumberland strata. Spirifer eriensis Grabau var. Geol. Soc. Am. Bul. 1899. 11:366, pl. 21, fig. 2a-b A variety of this species is more common in the upper Stroma- topora bed at Becraft than S. corallinensis. It is char. Big. 7 Spirifer eriensis var. acterized by a deep angular sinus with straight sides which diverge uniformly and regularly forward. It has narrow and more widely separated plications than S. corallinensis, and they become faint or obsolete in the upper part. A moder- ately strong plication occurs on each side of the sinus and 1044 NEW YORK STATE MUSEUM. another weaker one outside of this on each side. There are faint indications of a third one beyond that. The shell is character- ized by fine regular concentric lines which mark the edges of narrow imbricating lamellae. Fine radiating lines, interrupted by the concentric lines, are visible on well preserved specimens, giving a surface sculpture essentially like that of S. coral- linensis, S..vanuxemi and S. crispus. The ftotasos the brachial valve occasionally shows a faint iongitudinal depression. Measurement of specimens from Becraft mountain. ) Width Length Pedicle valve 1a 11 yb) oP) 13 ; : 11 ‘ e 15 at Pedicle valve of type specimen 10 8.5 Compared with the type from Williamsville, the present speci- mens, though generally larger, are very similar. The outline and median angular depression are alike in both. Only the lateral plications of the pedicle valve are more rounded and less widely separated in the Williamsville specimens than in the Becraft specimens. The number is also less, so that, ~ whereas in the Williamsville specimens there is a total of eight plications, only six can readily be made out in the Becraft speci- mens. The concentric surface striae are the same in both. The brachial valve of the Becraft specimens is somewhat more con- vex, with the plications a little more pronounced, particularly the ones next to the median fold. A single specimen from the Cobleskill of Schoharie (Am. Mus. 1856, with Atrypa lamellata) approaches closely to S. eriensis. The sinus widens regularly forward and the sides are flat; the bottom, however, is still rounded. Genetic relationship of the Spirifers of the S. crispus type The similarity between S. corallinensis of the New — York Manlius and Cobleskill and 8S. modestus of the Manlius! of Cumberland Md. has already been referred to. It REPORT OF THE STATE PALEONTOLOGIST 1902 1045 seems probable that S. corallinensis was derived from a smooth form similar to S. modestus,! though the chances of its having been derived directly from that form are slight. A type which answers more readily-the requirements of a radicle for this species as well as the others of this group, is Spirifer petilus Hall of the Niagaran beds of Waldron Ind. This species in the adult stage has all the characters of the young of S. crispus var. simplex and S. crispus, as pointed out by Beecher and Clarke2 S. corallinensis and S. eriensis are connected by intermediate forms. In some specimens from Becraft mountain, which show the adult char- acters of S. eriensis, the younger portion of the shell has all the characters of S. corallinensis with narrow shal- low sinus and obsolete plications. As the shell is exfoliated, it is not possible to say whether or not the plications are wholly absent in the young, as appears to be the case. The derivation of S. eriensis from 8S. corallinensis is then very clear, this being shown by morphogenesis as well as chronogenesis. In like manner it can be shown that S. vanuxemi was derived from 8S. corallinensis by an accelerated development of the plications, while the fold and Sinus were retarded. The most accelerated individuals of S. vanuxemi have, as already pointed out, a depression along the middle line of the fold which in extreme cases reaches the Deak. Phese three species, S. corallinensis, S. erien- Sis and S. vanuxemi, though occurring in the late Siluric beds, are all retarded in development with reference to the plications, when compared with S. crispus, which was derived from the same stock in the Midsiluric. In fact, these late Siluric species, if not known to occur above S. crispus, would be placed chronologically below or with that species Regarded however as retarded types, placed in an unfavorable environment, their more primitive characters are understood. 1Schuchert has recently pointed out [U.S. Nat. Mus. Proc. 1903. 26:413] that a number of the species referred to the Cumberland Helderbergian really belong to the Manlius horizon of that locality. Among these is S. modestus. 7N. Y. State Mus. Mem. 1. 1889. p.75. 1046 NEW YORK STATE MUSEUM S. petilus of the Waldron Siluric beds is succeeded genetically, though not chronologically, by S. crispus sim- plex, and this in turn by the normal S. crispus. There is also a strongly accelerated type in the Waldion beds which is characterized by a depression in the fold and rarely an eleva- tion in the sinus, and by angular plications. The normal New York type of S. crispus has strongly rounded but narrow plications, with a moderately deep, rounded sinus, which broadens strongly toward the front. This species was undoubtedly derived from the Waldron 8S. crispus by tnigration. Whether the pauciplicate rhombic type above mentioned is due to a direct immigration or to retardation of the normal S. crispus of New York can not be readily determined. The same may be said of S. bisulcatus Van- uxem, which is still more primitive, or more retarded. The results of our present studies in the phylogeny of these species may be summed up in the annexed diagram. REPORT OF THD STATE PALEONTOLOGIST 1902 WESTERN NEw YORK S. ertensis S. crispus< V S. crispus pauciplicatus V . Sbicostatus WALDRON IND. ose ee er eer ere oe eee es ow ® S. crispus beplicatus Sporifer crispus Spirifer crispus simplex a ee a eee eee ooo EASTERN NEw YorK S. vanucemi biplicatus S. vanucemi S. eriensis een S. corallinensis 1047 CUMBERLAND Mp. ETC, uvinkog S. vanuxemt S. corallinensis S. modestus cece eee eo wd ee Spirifer petilus > ? S. modestus ? UDLOBDUAT 1048 NEW YORK STATE MUSEUM Camarotoechia hudsonica sp. nov. Shell in form and size resembling C. neglecta of the . Niagaran, but differing in structural details. Pedicle valve less convex than brachial, with a pointed incurved beak. The valve is proportionally more convex at the beak, with the sides rather abruptly bending down. The valve broadens rapidly Fig.8 Camarotoechia hudsonica forward, having a triangular appearance. Lateral slopes below — the beak slightly concave, median depression beginning about halfway from the beak, at first faintly defined but becoming more pronounced toward the front, where it produces a marked — deflection of the frontal margin. It is never very much accen- tuated, but contains three pronounced angular plications which toward the front are separated by interspaces nearly twice their width. A plication of similar strength limits the depression on each side, becoming progressively fainter outward. Thus there are from four to five medially depressed ones. At the © beak the plications have the form of distinct threadlike, rounded striae. The concave lateral slopes are not plicate, but radiating striae have been observed in some specimens. Brachial valve uniformly convex, convexity greater than that of pedicle valve. Beak closely incurved. In the center of the valve four angular plications become more elevated from the center forward, the central two being most elevated, rising at times so much above the others as to give the fold a biplicate aspect. On either side of these are two fainter ones, with, gen- erally, indications of a third one near the margin. At the beak these plications are threadlike, rounded and uniform, except at the margin. ) Surface of valves marked by very fine, threadlike concentric lines, which are elevated and are equally strong on the plica- tions and interspaces. They are separated by spaces some- REPORT OF THE STATE PALEONTOLOGIST 1902 1049 what exceeding them in width. These lines are not visible in exfoliated specimens. This species is most nearly related to C. neglecta of the Niagaran of New York. It differs from that species in the more pronounced triangularity of the pedicle valve, the con- cavities on the lateral slopes below the beak, which give the valve somewhat the aspect of Rhynchotreta cuneata, the greater difference in convexity between the two valves and the fewer and less strongly pronounced lateral plications. The western representatives of C. neglecta have the median elevation and depression too pronounced, and the plications too sharp to correspond with our species, though the form and rela- tive convexity of the pedicle valve are more nearly like that of the present species. On the whole, the two species are readily distinguished. This species is abundantly represented in the upper Stromato- pora bed of the Manlius limestone at Becraft mountain. In the collection in the American Museum of Natural History containing some of the typical Coralline limestone fossils from Schoharie N. Y. this species is represented by a type more nearly like C. neglecta of the New York Niagaran. This has recently been described by Schuchert! as Rhynchonella litchfieldensis. The type specimen? erroneously figured as Atrypa lamellata, differs from our species as follows. The valves are more equally convex, the pedicle valve is less sharply constricted below the beak making the appearance less triangular. The median depression is faint, except near the front. It contains three plications which are like those of C. hudsonica. The character of the plications in general is like that of C. hudsonica, but there are about nine or 10 on each side of the depression, the outer ones fine but sharp. On the brachial valve of the four central elevated plications the median two are somewhat more raised. The number of lateral plications on each side is 10, the outermost fine and short. 1 Am. Geol. 1903. 31:67. ? Palaeontology of New York, v.2, pl.74, fig. 11h and i. 1050 NEW YORK STATE MUSEUM Width 10 mm, hight 9 mm, thickness 6 mm. [Am. Mus. eat. no. 1542 ] This compares quite well with a typical C. neglecta from the Niagaran of Lockport! except that the Lockport specimen has only six lateral plications on the pedicle and five on the brachial valve on each side. It differs as widely from the ordinary specimens of C. neglecta as does C. hudsonica. | Rhynchospira excavata sp.nov. General form and proportions as in R. formosa Hall, of the Helderbergian. The present species is however very con- vex in the umbonal region, and the cardinal slopes of both valves strongly excavated, a feature which recalls more nearly Camarotoechia than Rhynchospira. The beak of the pedicle valve is strongly incurved over that of the brachial. The apical portion is broken away in the only specimen known so far. The posterior lateral margins of the pedicle valve have a gently concave outline to almost the middle of the valve, beyond which they round regularly to the front. In the brachial valve the posterior lateral margins form a nearly straight line. A shallow median depres- sion begins at the beak of the pedicle valve and grad- ually widens forward, hav- ing in each stage of growth about twice the width of the spaces between the plications. The bottom of the depression is rounded, becoming flatter toward the front. It is margined on each side by a plication, which is somewhat weaker than those covering the remainder of the shell. The latter are sharply rounded and at intervals appear subnodose in the exfoliated shell, this feature being caused by strong concentric striae. There are in all nine plications on each side of the median line; two of these are very faint and short and occupy the depressed cardinal slopes. In the brachial valve a faint plication marks the center and corresponds to the depression of the pedicle valve. On each side of this are seven plications, the interspace Fig.9 Rhynchospira excavata * Palaeontology of New York, v. 2, pl. 57, fig lh, 1,0; Am. Mus. 1543, REPORT OF THE STATE PALEONTOLOGIST 1902 1051 between the first two plications being narrower than the three interspaces next succeeding. The seventh plication margins the cardinal slope, on which the eighth plication (corresponding to the interspace between the eighth and ninth plication of the pedicle valve) is undeveloped. A single specimen was obtained by the Columbia University field party from the upper Manlius of Mount Bob. The exact position of the specimen was not noted, but it probably belongs to the horizon of the upper Stromatopora beds of Becraft mountain. Whitfieldella cf. nitida Hall A single crushed specimen has the characters of the larger ‘individuals of this species. The greatest width appears to have been below the middle, the shell in this respect approaching W. intermedia in form. A consideration of this very meager fauna, which here occu- pies the very summit bed of the Manlius, shows its affinity to be with the Cobleskill limestone of Schoharie and the bullhead waterlime of Buffalo.t That it is a somewhat more advanced fauna than that of the Cobles- Fig. 10 pigs dele of nthide cp cteumtignen by the fact that the more specialized S. eriensis is the predominating type. The affinity of the fauna with that of the Tentaculite beds of the Manlius is shown by the occurrence of S. vanuxemi. Second.and third Stromatopora beds. Two feet below the upper Stromatopora bed is another about a foot thick but less con- tinuous than the first. The intervening beds are rather shaly. The Stromatoporas in this second bed are fragmentary, having been broken and worn to some extent before they were embedded. Where the Stromatopora fragments are wanting, - the rock is typical Manlius limestone with Leperditia alta. The Stromatopora appears to be the same as that in the upper bed. ' Hartnagel has shown the probable equivalence and continuity of the latter horizon with the Coralline or Cobleskill limestone of eastern New York. (J.M.C.) 1052 NEW YORK STATE MUSEUM Ten feet lower, or from 12 to 13 feet below the base of the upper Stromatopora bed, is a third one, averaging 2 feet in thickness. This has the aspect of a curly or concretionary rock, is of a darker color than the inclosing Manlius, and often highly crystalline. The structure of the Stromatopora appears on weathered faces only. The bed occasionally thins and then swells out again but does not exceed 2 feet in thickness. Its lower and upper contact surfaces are very irregular, and a certain amount of erosion (probably contemporaneous) appears to have occurred before the deposition of this bed. This is indicated by the wedging out of a 2 foot bed of Manlius. lime- Stone just below the bed, as shown in the annexed figure. Both the lower and mid- dle Stromatopora beds and the intervening rock are fis- sured and veined with cal- cite, which is often coarse- ly » crystalline: ‘As certain y,, Riz, 11 Diseam of pattie eae amount of slickensiding hag 0! the limestone layer beneath it also occurred, showing slight readjustment of the strata. In the southern end of the quarry over 40 feet of the Manlius were at one time exposed without reaching the “ Hudson river.” Contacts between Manlius and Coeymans. The contact between the Manlius and Coeymans, or the Siluro-Devonic contact, is shown in numerous exposures on the mountain. From the ex- posure at the head of the aqueduct in Greenport it can be traced westward for a short distance, when it disappears under. drift. Scattered ledges of both upper and lower rock allow its approxi- mate determination to the city quarry, where, as noted, it is again well shown. Beyond that it is traceable southwestward and southward in the cliffs and on the slope of the hillside, with some intermittances, though seldom with a well exposed contact, to the Jonesburg road. On the south edge of this, after crossing the meadow land, and halfway up the hill in a low cliff on the right, is a good exposure of the upper Manlius beds with the capping Stromatopora layer. The Coeymans is exposed in the road a short distance up the hill. The dip of the strata is 11°s.e., the strike n.30°e. For some distance southward from this REPORT OF THE STATE PALEONTOLOGIST 1902 1053 point the contact is not well exposed, but it soon appears again in the cliff, which sweeps out toward the Ancram road, and faces it for over a mile to the high bluff at fault 21. All along this side of the mountain, the Manlius, from its fine and uniform texture and the perfect jointage developed in it, produces gen- erally a vertical cliff. The Coeymans decomposes and makes more or less steeply sloping surfaces, which are generally used for grazing. The ledges project every now and then, making the slopes unfit for cultivation. In some places the upper part of the cliff is formed by the lower Coeymans, and at such points the bluff stands out boldly and is of great hight. The contact may be conveniently studied along the wood road which leads across the middle of the mountain, and branches off from the Ancram road a little over half a mile south of the cross road at Jonesburg. Where this road ascends through a little ravine, the cliff on the left contains from 10 to 20 feet of Coey- mans in the upper portion of its face, behind which the remainder of the Coeymans forms a slope to the foot of the cliffs formed by the New Scotland. Only the upper portion of the Manlius is well exposed along the cross mountain road. It is compact and finely stratified and contains Leperditia alta in its upper portion. 7 On both sides of the valley, bounded by faults 21 and 20, the contact between the Manlius and Coeymans is well exposed in the face of the cliff. No Stromatopora beds have been observed. Since, however, the actual contact can be seen only in a few points, owing to the steepness of the cliffs, it is not possible to say whether this bed is absent over the entire western face of the mountain or not. Near the junction of the Ancram road with the southern road, the Manlius passes below the surface and does not appear again till the schoolhouse, half a mile farther east, is reached. Here the Manlius is seen just south of the road, standing vertically, _the contact with the Coeymans, though not exposed, being close _ to the southern margin of the road. Just east of this, fault 18 has thrown the contact 600 feet to the south, the dip of the strata being still vertical or steeply inclined. From this point 1054 NEW YORK STATE MUSEUM eastward rocks are exposed within a few feet of the contact, so that the latter can be readily traced, with some interruptions, to a few hundred feet beyond the central mountain (Newman) road, after which no exposures of the Manlius have been observed for over half a mile northeastward. Hence the actual contact of the Manlius and Coeymans can not be determined, but it can be readily inferred from the positions of the contacts of the higher formations. Beyond this the contact can be easily ascertained, being for the most part actually exposed in the face of the cliff, or at least indicated by rock exposures within a few feet on each side of the actual contact. 7 The Stromatopora bed has not been observed along the eastern face of the mountain, but is found in the outcrops along the southern portion. For the most part the outcrops of the Manlius appear as a narrow strip on the map. This is due to the fact that this forma- tion, when but slightly inclined, generally makes a cliff, owing to the uniformly compact character aud perfect jointing of the rock. When vertical or steeply inclined, a cliff may or may not be formed; in any case the exposure does not much exceed in width the thickness of the Manlius as found at Becraft. Only © along the northern end a broad belt of this rock is exposed, for here the inclination is very gentle (10° to 20°), while the slope is likewise a gentle one and for the most part drift-covered. The absence of the usual cliff here may be accounted for by glacial erosion, this being the side most exposed to the force of the ice. 4 THE COEYMANS LIMESTONE This is a compact, finely crystalline, generally dark colored | limestone. Fossils are abundant only in the upper layers, the most characteristic species being Atrypa reticularis, Gypidula galeata and crinoid stems. Layers of chert are not infrequent, and in some outcrops form a constant and characteristic feature. There is sufficient argillaceous matter -in this rock to give it the characteristic odor when breathed on. The organic fragments are large enough to be recognizable, though there is also a considerable admixture of flourlike REPORT OF THE STATE PALEONTOLOGIST 1902 1055 material. On the whole, the rock may be considered an argil- laceous calcarenite.t The rock is readily distinguished from the Becraft limestone by its texture and color, but not so readily from the Port Ewen. The total thickness of the Coeymans is about 45 feet. The lower 20 or 25 of these are generally massive bedded, often crinoidal, and form commonly a vertical cliff in conjunction with the underlying Manlius limestone. The upper portion of the Coeymans is thinner bedded, with more or less shaly layers separating the beds, and this is expressed in the topography by a sloping bank, with occasional low, reeflike rock ridges mark- ing the strike of the strata. This feature is most readily observed on the west side of the mountain, at the top of the cliff facing the Ancram road between Jonesburg and fault 21. The fossils are most abundant in this upper shaly portion, and to some degree these beds form a transition to the New Scot- land above. Atrypa reticularis is everywhere com- mon, while Gypidula galeata is also frequent in these beds. With these in the upper layers occurs rarely Spirifer macropleurus, showing the beginning of the New Scot- land fauna. The following is a list of the fossils of the Coeymans lime- stone of Becraft mountain, obtained chiefly from the upper beds. 1 Monotrypa tabulata (Hall). Not very common. 2 Favosites helderbergiae Hall. Several speci- mens were found in the top beds of this limestone. Some speci- mens were also found in the lowest beds. 3 Enterolasma strictum (Hall). Not uncommon in the upper beds. Poa Sitiilipo ha wtert a, Hall... Abundant.. 5 Roemerella grandis (Hall). A specimen having the size and form of this species. The surface is covered with very irregular concentric striae, and extremely fine radiating lines are visible only between the concentric striae. 2 Grabau. Science, n. ser. Feb. 20, 1903. p. 297. 1056 NEW YORK STATE MUSEUM 6 Lingula rectilatera Ball. A single specimen showing form and convexity of this species. 7 Dalmanella subcarinata Hall. -A single speci- men. | . 8 D. perelegans Hall. Occurring with Gypidula galeata. | 9 Leptaena rhomboidalis (Wilckens). Abundant. 10 Stropheodonta varistriata Conrad, var. arata Hall. Not an uncommon form. | 11 8. varistriata var. A Specimen between the spe- cies and the variety arata. 12 Strophonella headleyana Hall. A specimen in the crystalline limestone with the features of this species. 18 S$. leavenworthana Hall. 2 specimens. 14 Cyrtia dalmani Hall. 1 specimen. 15 Strophonella a (Conrad). Sev- eral specimens. 16 Spirifer perlamellosus Hall. A number of specimens showing variation in length and width and occurring in the more shaly or transition portion of the upper Coeymans. 17 S. cyclopterus Hall. Several specimens referred: to this species. 18 S. macropleura Conrad. In the calcareous portion of the upper Coeymans, i. e. the transition beds, a Specimen -was found showing the characteristic features: with it occurs Gypidula galeata. 19 Unecinulus nucleolatus (Hall). A single speci- men. 20 Eatonia peculiaris Conrad. A perfect specimen. 21 E. medialis Conrad. Rare but typical. | 22 Atrypa reticularis (Linné). Common. 23 Gypidula galeata (Conrad). Abundant. 24 Anas trophies ver neurin = Hall = Aecsmele char- acteristic specimen from the upper part of the limestone. 25 Meristella princeps Hall. A single large bra- chial valve. 26 Pterinea (?) textilis (Hall). 1 specimen. REPORT OF THE STATE PALEONTOLOGIST 1902 1057 at Platyceras platystoma Hall. A’ specimen with the general aspect of this species. 28 P. subnodosum Hall. 1 specimen. 29 P. cf. retrorsum Hall. 2 specimens agreeing in general with this species. se uneuiforme ? Hall. 2 specimens having the form of this species, but lacking the full number of plications. 31 Dalmanites micrurus (Green). Rare. Sa Da cl. pleuroptyx (Green). 33 Phacops logani Hall. A head in the fine compact limestone, probably the transition beds of the Coeymans. With it occurs Gypidula galeata and Monotrypa. _ The following species were obtained mainly from the upper layers of the Coeymans at Mount Bob. 1 Favosites helderbergiae. Basal beds. 2 Rhipidomella cf. oblata: Hall. 3 Stropheodonta varistriata (Conrad). Associ- ated with Uncinulus pyramidatus in the crystalline limestone. 4 SS. varistriata var. arata-_ Hall. 5 Spirifer cf saffordi Hall. 2 specimens with the characters of this species. 6 S. perlamellosus Hall. 1 specimen. fect, OCLoplicata Hall.. With no. 13. 8 Uncinulus pyramidatus (Hall). With 3, 12, 13 and 15. 9 U. ef..mutabilis (Hall). Young; 2 specimens. 10 Rbhynehospira formosa Hall. 2 specimens. Mm Rhynechonella altiplicata. Hall.: With 14. 2 Meristella prineceps Hall. 13 M. laevis Hall. 1 specimen. 14 Gypidula galeata. Common. im Aviculopecten spinulifer (7) Meek & Wor- then. A specimen of a right valve more convex than that fig- ured by Hall, but showing form and surface characters of that species. : 16 Dalmanites cf. micrurus Conrad. 1058 NEW YORK STATE MUSEUM From these lists it will be seen that a considerable number of species commonly referred to the next fauna, i. e. the New Scotland, are found in the upper Coeymans. In these same beds Gypidula galeata is common, thus showing well their transitional character. ; All of this series contains crystalline limestone, while the overlying New Scotland contains no pure limestone. The finely crystalline character of the Coeymans also distinguishes it read- ily from the Manlius, which is generally compact. About the middle of the eastern face of the mountain, where the beds are all on end, the thickness of the Coeymans measured across the strike is 42 feet. [See postea] The most accessible exposure of the lower and upper contacts of the Coeymans is on the middle transverse mountain road leading off the Ancram road a short distance south of the old glue factory. One of the best places to obtain the fossils of this rock is at the extreme southwest corner of the mountain on the north side of the road leading southeast. The rock here is f exposed at the road side. 5 NEW SCOTLAND SHALES These are thin bedded, argillaceous to silicious rocks, in which a variable amount of calcium carbonate is present. Usually this is insufficient to allow the rock to be affected by acids, there being no, or but very feeble, reaction on applying strong HCl. Fossils are abundant but usually only preserved as molds, though, when the rock is freshly broken, the shell is still found remaining. | The following list comprises the species obtained from these beds at Becraft mountain. 1 Enterolasma strictum Hall. Rhipidomella tubulostriata Hall. Rare. R. eminens Hall. Several. R. oblata Hall. Several. Dalmanella perelegans? Hall. D. cf. subcarinata Hall. Rare. 7 Schizophoria cf. multistriata Hall. A speci- men showing form, convexity and striae of this species. aS oO FP WD WLW REPORT OF THE STATE. PALEONTOLOGIST 1902 1059 8 Orthothetes radiatus Fischer. Rare. 9 O. woolworthanus Hall. Common. - 10 Stropheodonta becki Hall. Common. 11 Strophonella headleyana Hall. Common. 12 Leptaena rhomboidalis (Wilckens). Common. 18 Spirifer macropleura (Conrad). Common. 14 S. perlamellosus Hall. Common. 15 EHatonia peculiaris Conrad. Rare. 16 E. medialis Vanuxem. Frequent. 17 Meristella cf. arcuata Hall. Rare. 18 M. subquadrata Hall. Rare. 19 Anastrophia verneuili Hall. Rare. 20 Diaphorostoma ventricosum (Conraad). Large individuals. | 2) Platyceras bisulcatum MHall. 22 P. ventricosum Conrad. 23 P. gebhardi Conrad. 24 Platyceras sp. Several uncoiled forms which repre- sent the next stage after P. gebhardi cf. P.magnificum of the Oriskany. 25 Dalmanites micrurus Green. Frequent. 26 D. nasutus Conrad. Frequent. 27 D. pleuroptyx? Green. A single specimen, some- what distorted by cleavage across the bed, lying in such a position that the compression shortened and widened it. In the quarry face of the Jonesburg stone-crusher, about 25 feet of the New Scotland beds are exposed. They are quite cal- careous and heavy bedded where freshly broken. In the lower portion the characteristic fossils are common, i.e. Spirifer macropleura, Strophonella headleyana, Stro- pheodonta becki, Leptaena rhomboidalis, ete. The best measurement obtained of the thickness of the New Scotland was 68 feet. This was taken just north of fault 14 where the whole formation is exposed on end between the Coeymans and the Becraft limestones. On the hillside above fault 21, the measured thickness was 70 feet to 75 feet. Wher- ever these beds are but slightly inclined, they form a series 1060 © NEW YORK STATE MUSEUM of steps in the topography, with a steep cliff due to the well de- veloped joint planes, and a gentle slope down the bedding plane. Not infrequently a number of such steps are met with in crossing the outcrop from the Coeymans contact to that of the Becraft above. These may vary in hight from a few feet to 30 or more feet, but generally they range between 10 feet and 20 feet in hight. It is this steplike arrangement which caused Mather to believe in the existence of block faulting [fig. 1, p. 1031]. 7 The New Scotland is the boulder formation of the region. Blocks of it are found everywhere scattered over the fields, or piled up in fences. Along the eastern side of the great Oriskany “bottom” on the western half of the mountain, a wall of these blocks occurs. though there is no outcrop nearer than half a mile. Near the middle transverse mountain road, these bottoms are strewn with boulders of New Scotland, which also are abundant on the side of the Esopus hill east of the bottom. These frag- iments might easily mislead one to look for an outcrop of the New Scotland in this locality. . 6 BECRAFT LIMESTONE This is a light gray, coarsely crystalline limestone (calcarenite) becoming in places a shell marble. Certain beds, specially near the bottom, are composed of crinoid joints, and the basal por- tion of the calyx of Aspidocrinus scutelliformis, while near the top shells of Gypidula pseudogaleata locally make up the rock. The fossils, though numerous, are not very rich in variety. The most abundant and characteristic types are Spirifer concinnus, usually small, Gypi- dula pseudogaleata, Atrypa reticularis and Uncinulus campbellanus. The following is an anno- tated list of the species found in this rock. I. “Pemnes ted lan sp. 2 Schizophoria multistriata Hall. Not very common. 3 Leptaena vhomboidalis (Wilckens). 4 Spirifer concinnus Hall. Small individuals with the character of the young of this species are common in the limestone. The sinus of these specimens is angular, and there ae, REPORT OF THE STATE PALEONTOLOGIST 1902 1061 are five or more plications on each side. An average individual measures 11 by 15 mm and has about six or seven plications on each side of the median sinus. A larger individual measures 18 by 26 mm and shows the characteristic high area and sloping cardinal sides of this species. It has about 10 plications on each side of the sinus. This is the most characteristic species of this limestone, but most of the individuals are small, with immature characters. 5 Spirifer perlamellosus Hall. Several speci- mens showing characteristic form and plications but only occa- sionally showing the concentric lamellae. 6 8S. cyclopterus Hall. A few specimens showing form and character of plications of this species. 7 Rhynchospira formosa Hall. 2 well marked individuals. 8 Uncinulus campbellanus (Hall). A common species in this limestone. 9 U. nobilis Hall. A number of more rounded and more coarsely plicate individuals from these beds are referred to this species. They do not have the characteristic lateral depres- sion of the cardinal margins. 10 Atrypa reticularis (Linné). A robust variety is common. 11 Meristella prin ce ps Hall. A single specimen. 12 M. arcuata Hall. Several internal molds and a shell with the characters of this species. 138 Eatonia medialis Vanuxem. A single valve re- ferred doubtfully to this species. 14 Trematospira perforata Hall. A single char- acteristic specimen of this species was obtained from the weathered portion of this limestone. 15 Gypidula pseudogaleata Hall. Abundant. 16 Rensselaeria mutabilis Hall. A single speci- men. 17 Platyceras cf. gibbosum Hall. This specimen may have come from the New Scotland layers. 18 Aspidocrinus scutelliformis Hall. Abun- dant in the lower layers of the limestone. 1062 NEW YORK STATE MUSEUM The following species were obtained from the top layers of the Becraft limestone: 1 Monotrypa sphaerica (Hall) Leptaena rhomboidalis (Wilckens) Spirifer concinnus Hall Rhynchospira formosa Hall Katonia medialis Vanuxem Gypidula pseudogaleata Hall Spirifer sp. These form a transition to the Port Ewen fauna. Just above the stone-crusher quarry at Jonesburg an excava- tion in the hillside shows the basal members of the Becraft. The beds here are 6 inches to a foot in thickness, and separated by shaly layers. The dip is 11° into the hill; the actual contact is not exposed however. In the old Fred W. Jones quarry, nearly the full thickness of the Becraft is shown in the quarry face opposite the junction of the quarry road with the Jones- burg cross road. About 6 or 8 feet of the lower beds are con- cealed, which, together with the thickness exposed in the cliff, about 35 feet, make a total thickness of between 40 and 45 feet for the Becraft limestone. The Port Ewen appears a short dis- tance south of the edge of the quarry, the surface slope here | | being with the dip of the strata. Hence the above estimate of | the thickness is very close. A similar thickness of 45 feet was - obtained by measurement of the outcrop on the east side of the mountain, where the strata stand vertically. The limestone has been extensively quarried in the past for fiux, the amount of Ca Co, being nearly 92%. The following analyses were published by Ries in his report, the Limestones of New York and their Economic Value. AD Oo FP & LD ATG oe cee gs ph aaa es eeu, a mdaey cid a en een 51.4 ee Lime: carbonates). dca o5+cda-2us dee Seen ee 91.7 Carbon vox: yo ce Sisicte he a eee eae 49.191: = 35 ee Ma gnesiiim: CarDOmate@ oo. clin ncece oh fuga Sig aan aa ie E 3.51 Ma mesa si oinie «5 ise att Set id ae ee eee Dis Lend os cfetringal 1N. Y. State Geol. 17th An. Rep’t 1897; N. Y. State Mus. 51st An. Rep’t, 2:431. REINER VS Yarbrys1s oie lees) ba lela oS es a eet G25) Ae OL 8 SR ee es ee itabe8t .55 ee eee Seba oy ndy sys aid ay 9 Ssoehcata (el o's 1.842 1.89 OU ree a .145 .049 NOUN Mig) ie ofc op giclee BG's bd sa Kiso ate « .149 022 MP eo. 1) debgh eae Wk ees 1 Ove b: dation 107.685 98.731 7 PORT EWEN (KINGSTON) BEDS In his sections of the region about Kingston and Rondout Davis! described a series of shaly limestones, lying above the Becraft limestone, and similar in character and fossil content to the Shaly limestones (New Scotland beds) underlying the Becraft. To these upper beds Davis gave the name of Upper Shaly limestone which was later on changed to Kingston beds by Clarke & Schuchert.2. This term was, however, preoccupied by various authors for formations of Precambric, of Siluric and of Pleistocenic age, and Clarke has since proposed the name Port Ewen beds, from the town opposite Rondout, near which these beds are best exposed. The thickness of these beds near Port Ewen station on the West Shore Railroad is recorded as 222 feet. Van Ingen and Ruedemann divided them into 18 subdivisions and made exten- sive collections from these, which have been published by Clarke.* On the authority of these collections, Clarke states that “the fossils of all its layers are those of the true New Scotland lime- stone faunas, the contents of the higher layers varying little from those of the lower.” As no such formation seemed to occur at Becraft mountain, where the normal succession of strata is undisturbed and clearly exposed, I visited Rondout hill in com- pany with Dr John C. Smock, in order to study the formation at the type locality. Accompanied by Mr P. E. Clark, the mining engineer of the cement works, I made a careful examination of critical points on the hill, expecting to find the lower Shaly beds 1 Am. Jour. Sci. 1883. 26:389. "Science. Dec. 15, 1899. *Qriskany Fauna of Becraft mountain, p. 73. 1064 NEW YORK STATE MUSEUM repeated by overthrust faulting. Above the Becraft limestone © and below the beds pointed ont by Mr Clark as “ Upper: Shaly,” and so mapped by Davis and Darton, the Coeymans limestone was found in full force with characteristic Gypidula galeata and Atrypa reticularis, as well as the chert beds characterizing it as Becraft. Above the “Upper Shaly,” after careful search in the woods, the typical Becraft limestone was found, which in turn was overlain by a darker, fine grained limestone identical in character with the beds lying between the Becraft and Oriskany at Becraft mountain. Above this was found the Oriskany. On extending our observa- tions, Mr Clark pointed out a spot where the Becraft, inclined about 50°, was quarried below, and the Rondout waterlime, inclined at 42°, was quarried above it. On examining the contact between the limestones below the point where the Coeymans was found overlying the Becraft, in the roof of an old quarry in the latter rock, it was found that the line of Supposed overthrust was clearly marked by extensive slicken- siding of the adjoining strata.! A subsequent visit to this hill in company with Dr Ruedemann showed the essential correctness of the interpretation of the structure, but it was found that the thickness of the beds lying between the Becraft and the Oriskany was greater than at first supposed, Dr Ruedemann measuring 110 feet. A visit to the section in the West Shore Railroad showed a ereat thickness of the Upper Shaly beds between the Becraft and the Oriskany. The section made by the railroad however is, as pointed out by Mr Clark, a diagonal one and numerous small faults occur in it so that the actual thickness would be less than 222 feet, as recorded by Clark. Since the interval between the Be- craft and the Oriskany can be readily measured on Rondout hill, though the beds occupying that interval are poorly exposed, it !'No ‘ Upper Shaly ” beds are recorded by Davis in his sections and descrip- tions of the ‘‘ Little mountain region”’ east of the Catskills. His map covers an area of about 10 miles in length and throughout this the Oriskany, where present, rests directly on the 120 feet of limestone which he referred to the Upper Pentamerus (Becraft). The upper part of these undoubtedly represents the Port Ewen of {Becraft. | 3g 2.¢4ia J« coad 2S REPORT OF THE STATE PALEONTOLOGIST 1902 1065 seems probable that the Port Ewen section, which is not more than a mile and a half south of the former, contains not much more of these beds. Darton estimates the thickness as 125 feet in the central and southern portion of Ulster county, and states ‘that it decreases northward to 30 or 35 feet in the Saugerties region, near the Greene county linet The Upper Shaly beds of the Port Ewen section have a thickness of from 100 to 200 feet, but except along the roadside, they are poorly exposed on Kings- ton hill. They, together with the Becraft and the repeated Lower Shaly, were mapped by Davis and Darton as Upper Shaly, while the characteristic fossils cited by these observers were obtained beyond doubt from the repeated Lower Shaly beds, for Spirifer macropleura and Orthothetes radiatus cited by Davis and Darton as characteristic of the Upper Shaly do not appear in Clarke’s list of these beds as exposed in the Port Ewen section. At Becraft mountain these beds are well shown. They are dark crystalline limestones recalling the Coeymans limestone. They crop out in a series of steps with a total thickness of not over 25 feet. They are particularly characterized by the Monticuliporoid Monotrypella tabulata, which may be easily recognized by the transversely wrinkled aspect of the corallites. This species is however not restricted to this hori- zon, being also known in the Coeymans limestone. The best exposures of the Port Ewen beds are along the quarry road from the old Jones quarries to the transverse mountain road. Here the thickness can be best determined, and the char- acteristic fossils obtained. The bluffs here rise up to 15 or 20 feet in hight, and above them there is a continuous slope east- ward, conformable to the dip of the strata, to a low swampy meadow, where fragments of Oriskany limestone indicate that the contact is near. Allowing for a slight addition above, and a similar addition below to the contact with the Becraft, I do not think that the total thickness of the Port Ewen at Becraft moun- tain will exceed 25 feet. 1N. Y. State Geol. 13th An. Rep’t. 1894. p. 304. ers me SERS ae SERGE ons a ee hs Bot vee ee ee 1066 NEW YORK STATE MUSEUM In lithic character the Port wen beds of Becraft resemble the Coeymans, and, like these beds, they contain more or less chert. The similarity is emphasized by the occurrence of Monotr y- pella tabulata in both. | The paleontology of this limestone still needs a careful study. | The following annotated list represents the species found in a brief examination of this rock during the progress of mapping the contacts. Care was taken to obtain them from character. istic outcrops, so that there could be no confusion with over- lying or underlying strata. | Fossils of the Port Ewen beds of Becraft mountain 1 Monotrypella tabulata (Hall). Abundant, par- ticularly in the upper beds. : 2 Cladopora cf. styphelia Clarke. 2 specimens which resemble this species, but have smaller apertures at in- tervals surrounding, or nearly so, the larger; found in the upper beds. 3 Orthothetes becraftensis Clarke. A _ few specimens of this Oriskany species were found showing charac- teristic form and surface markings. 4 Leptaena rhomboidalis (Wilckens). Middle beds. 5 Stropheodonta gp. 6 S. (Leptostrophia) magnifica Hall. In the middle Kingston beds are some specimens which may readily be referred to this species. The muscular scar is less sharply marked than in Str. becki, they are larger and more | spreading, and there are four stronger diverging ridges on each side of the central one. The punctate structure is well marked, the punctae being disposed in rows between the striae. No concentric wrinkles have been seen in any of these specimens. These specimens appear to be intermediate between S. becki | and true 8S. magnifica. A large typical pedicle valve, hav-- ing a maximum width of nearly 75 mm, was obtained from the lower beds just overlying the typical Becraft. A moderate sized specimen was obtained from the upper beds. 7 Spirifer concinnus Hall. A large pedicle valve, with a width of 40 mm and a hight of 25 mm, was obtained from REPORT OF THE STATE PALEONTOLOGIST 1902 1067 the middle beds; the width of the sinus at the anterior margin is 10 mm, and there are 13 or 14 plications on each side of the sinus. 8 S. econcinnus Hall. Small specimens like those found in the Becraft beds are not uncommon in the middle beds on the quarry road. 9 S. cyclopterus Hall. A large specimen was obtained from the middle beds on the quarry road. 10 ‘S. sp. 11 S.perlamellosus Hall. Middle beds; rare. 12 Rhynchospira formosa Hall. 1 specimen. 18 Eatonia peculiaris Conrad. Middle beds; rare. 14 Meristella typus Hall. A single specimen show- ing form and concave or flattened cardinal margins of this spe- cies, was found in the upper beds. According to Schuchert this Species occurs only in the Manlius of Cumberland Md. 15 M. ef. princeps Hall. Middle beds. 16 M. sp. 17 Rensselaeria gp. Peat yeceras cf. trilo-batum Hall. Middle - beds. A consideration of this list shows that these beds have a transitional character from the Becraft to the Oriskany of Becraft mountain. This is shown by the occurrence of charac- teristic Oriskany and Becraft species side by side as well as by the intermediate character of some species. Oriskany species are Cladopora styphelia, Or- enothetes beceraftensis, Stropheodonta magnifica and EHatonia peculiaris. Affinities with the Becraft limestone are shown by Spirifer con- c€innus and with that and the lower beds by S. cyclop- terus, S. perlamellosus, Rhynchotrema for- mosa, etc. A more extended collection would probably show more tran- sitional forms in the lower and middle, and other Oriskany Species in the upper beds. i068 NEW YORK STATE MUSEUM 8 ORISKANY BEDS These are silicious limestones, often with an abundance of chert, the fossils being mostly silicified and weathering out readily. Says Clarke: ! These strata, highly silicious, hard, dark limestones, have been most favorably exposed to decomposition, and in consequence the calcareous matter_has been largely leached out for a con- siderable depth on all exposed surfaces, only a porous residuum remaining. This light, rusty and firm rotten stone retains the external and internal casts [molds] of the fossil remains with which it is filled, in exquisite detail and forms excellent material for study. Only by hastening nature’s process with acid can the fossus be made out from the black and cherty or Le calcareous cores of this rock. The fauna of this formation was fully described and illustrated by Clarke. He summarizes it as follows: ? Of the 94 clearly defined species of this fauna, 38 represent ex- pressions of species which began their existence in Helderbergian times; on the other hand, but 18 of the species of the fauna con- tinued their existence, or appear to be represented by closely - allied forms beyond the close of the Oriskany sedimentation. 29 are represented in the earlier known fauna of the arenaceous beds of the Oriskany. ? The only satisfactory exposures of the Oriskany bed in situ are, first, on the middle mountain road (Newman road) along the western side of the road between the quarries of Becraft lime- stone on the north and the stream which crosses the road near the contact of the Oriskany and Esopus on the south; and second, in the field to the east of this, where the beds are brought up in little folds. The best collecting grounds for the weathered out fossils are in this same field, north of the flat bottomed meadow ground, and in the fields west of the swampy area which marks the Oris- kany-Esopus contact on the western side of the mountain. One of the most accessible localities is at the crossing of the: middle transverse mountain road over this stream. Weathered out Oriskany fossils are also found at the northern outcrop of the Oriskany on syncline no. 2 and occasionally along the stream following the Oriskany outcrop between faults 15 and 17. The 1 Oriskany Fauna of Becraft Mountain, p. 12, 13. EOE CU Os Cle REPORT OF THE STATE PALEONTOLOGIST 1902 1069 rock with its fossils weathered out in relief is seen in a little hillock in the southwestern part of the mountain, where it has been brought up by fault no. 19. [See map] It is not possible to give the exact thickness of this formation at Becraft. It can not be more than a few feet, and is probably not much more than a foot. It grades below into the Port Ewen limestone, but is abruptly overlain by the Esopus grits. The con- tact between the Oriskany and Esopus is everywhere marked by low swampy ground and by the existence of stream beds. A glance at the map will show that the streams have all become adjusted to the Oriskany bed, not so much because this rock is a softer one, | for, though commonly decomposed, the silicious portion stands out in relief. It is rather due to the fact that the overlying Esopus shales break up readily into a fine gravelly soil, which is easily removed by the streams. The Oriskany and Port HKwen act as a guiding plane along which the streams work downward. The few departures from the characteristic method are explain- able by local conditions of folding or faulting. 9 and 10 ESOPUS AND SCHOHARIE GRITS These are dark chocolate-colored, gritty shales, with a com- bined thickness of about 300 feet, of which about one third is considered as belonging to the Esopus. The dividing line is drawn on lithic characters, which are chiefly expressed in topo- graphic features. The Esopus readily crumbles into small cubical fragments under the influence of the weather, and hence presents rolling surfaces, which commonly constitute the best farming sround of the region. The Schoharie, on the other hand, resists the weather more easily, but generally has its cleavage planes well developed by the weather. These are commonly at a high angle, and their presence obliterates the original bedding planes. The topography of this rock is rugged, with numerous ledges, and hence is generally left wooded: The best exposure of the Esopus is above the contact line with the Oriskany on the west side of the mountain. Here in the hillside above the stream, ledges of the Esopus are visible. The Schoharie may be studied almost anywhere over the area of its outcrop. Clarke has recorded the 1070 NEW YORK STAT® MUSEUM following species from the outcrop of the Schoharie at the junc- tion of the Newman road with the middle transverse mountain road.t | Dalmanites anchiops, Phacops cf. bombi- frons, Coelospira cf. camilla and Chonetes ef. arcuatus. These he considers sufficient to identify the ages of the beds. 11 ONONDAGA LIMESTONE This is the highest formation of Becraft mountain. It occu- pies the top of a ridge in the southeastern portion of the mountain and is of very limited extent. The portion of the bed remaining is involved in syncline no. 2, the eastern limb of which is turned — up vertically. The upper part of the rock is very cherty and weathers with irregular surfaces. The limestone is light gray in color and finely crystalline. Fossils are not readily found, but Clarke has recorded Spirifer raricosta and Zaphrentis from the upper part, and from the lower, chert-free beds Od o0n- tocephalus' selenurus, Spirifer varicosus, Atrypa reticularis, Leptaena rhomboidalis, Streptorhynchus pandora, Chonophyllum, Zaph- rentis, Favosites and Stromatopora or Fistulipora.2 Orthoceras and EKuomphalus were also noted in the upper beds. The total thickness of the Onondaga is not over 25 feet and is probably nearer 20 feet. } The outcrops of this rock are most easily approached from the eastern road by striking into the fields after crossing the little stream from the Oriskany depression, which here breaks across the strata to join Claverack creek. It may also be approached from the Newman road by following the Oriskany depression northeastward and ascending the hill. The approach over the Schoharie is difficult on account of the wooded and rough char- acter of the land. Loc. cit. p.14. * Loc. cit. p.15. REPORT OF THE STATE PALEONTOLOGIST 1902 1071 TECTONIC FEATURES Becraft mountain is an isolated remnant of the Helderberg mountains and partakes of the general structure of the Appa- lachian system of which it forms a part. It is not the only remnant of the Helderbergs on the east of the Hudson river, for a few miles to the northeast lies Mount Bob, which is an abbreviated edition of Becraft having suffered all but complete destruction by erosion. Whether Becraft mountain represents a fault block of the Helderbergs dropped down among the “Hudson river” strata and so preserved from erosion, or whether its low lying position with reference to the Hudson river beds Surrounding it, is due to the fact that it forms an axis of a particularly deep syncline, which during the peneplenation of the surrounding country was” too low to suffer erosion, is not easy to determine. Certainly, if the strata on the west of the mountain were continued upward at the same angle with which they now dip into the mountain, they would pass above the highest point of Mount Moreno, which is the highest mass of Hudson river strata lying between Becraft and the Helderbergs. The fact also that Mount Bob, lying in the direction of strike of the Becraft strata, has a synclinal structure, indicates that they are one and the same part of the low lying synclinorium. The main synclinal axis (no. 1) of the Becraft mountain synclinorium runs about through the center of the mountain. The western limb is simple, but the eastern limb is strongly folded and faulted. Two anticlines (no. 1 and 2) and two more synclines (no. 2 and 3) are readily traceable over the eastern half of the mountain. The eastern limb of the third syncline (no. 3) forms the western limb of a third anticline (no. 3), this anticline being complete in only one locality [see sections 12-15], where it is followed. eastward by another syncline (no. 4) and finally by a small symmetric anticline (no. 4). Besides these there are several minor folds between the major ones. The principal folds (anticlines 1, 2 and 3) are strongly asymmetric, their western limbs varying from steeply inclined through perpendicular to strongly overturned. In addition to this, the 1072 ; NEW YORK STATE MUSEUM eastern side of the mountain is strongly diversified by numerous faults. The axes of the folds approach each other toward the southwestern end of the mountain, where they are cut off by a transverse fault (no. 18). As might be expected, the folding is likewise more intense in this locality, as will be seen by a comparison of sections 21 and 25. The general pitch of the Becraft syneline is toward the southwest. But there is also a local pitch to the northeast in the strongly folded southwestern area. Thus a_basin- shaped appearance is produced, with the suc- cessive rimming around of the outcrops of the lower about the higher strata. The faulted district begins on the north- - eastern corner of the mountain. Here, as shown by the following section [section 3], the throw is comparatively slight. Fault no. 1 is a gravity fault the hade of which could not be accurately determined, but appears to be vertical; the strata are abruptly turned up at the downthrow side. This feature is very readily seen in the hillside. . The amount of vertical displacement here is about 20 feet. Fault no. 2 is a thrust fault with a very oblique fault plane, the hade being about 70°. The vertical throw is from 70 to 80 feet and the horizontal displacement about 800 feet. From the fact that the fault is traced down the hillside, it appears curved on the map. Fault no. 3 is a gravity fault, a block east of it having dropped down. It can be fol- lowed along a wood road in a depression, with the Coeymans on the east and the Man- lius on the west of it, both dipping west- ward, the Manlius at a greater angle. The S}[NB} 9014} SatMoyYs ‘UIV{UNOU 4ye1Neq Jo UOTZIOd ysvey}IOU JO UOTIVES GT “Sli REPORT OF THE STATE PALEONTOLOGIST 1902 1073 eastern face of the fault block is mainly a steep cliff, with the contact between the Manlius and Coeymans part way down the cliff. The Manlius is here much jointed, with vertical joints which on weathering give the aspect of vertical bedding. Shortly before reaching the bend in the wood road, where it leads off to the Becraft quarries, a sink hole of moderate depth is met with. There are several of these on Becraft, which point ‘to a more or less cavernous condition of the low lying limestones. Faults 4 and 5 appear to bound the keystone of a small anticlinal fold, which has collapsed at the center. The strata on either side of the central fault block are dipping away from it. Fault no. 5 also permitted a lateral displacement of the blocks. South of fault no. 5 the surface rock is the Coey- mans, which, together with the dip of the strata, would give about twice the known thickness of the Coeymans. It seems therefore highly probable that another fault (no. 6) runs through the center longitudinally. The throw is of course not so great in this second block, since no Manlius has been brought to light. Fault no. 6 must be regarded as the continuation of fault no. 3. Both of these faults are earlier in date than fault no. 5. Fault no. 7 is another gravity fault with the downthrow on the south- eastern side, and the strata of this portion steeply turned up on the fault plane. West of this the strata are strongly folded, as shown in section 6. _ Fault no. 8 is more of the nature of a breached anticlinal fold, though a slight displacement seems to have occurred at the axis of the fold, where a small stream runs from the mountain side. All of these displacements and extra folds die out toward the southwest, as shown in section 12a, where only a single fold (anticlinal 1) can be made out. — Unlike the preceding faults, which mostly had a uniform direction (about n. 40 e.) or else were parallel to the strike. fault no. 9 has a direction a little south of east. It cuts off the end of syncline no. 2, causing a partial repetition of some of its strata, i. e. Becraft and New Scotland. The downthrow in this case is on the north side of the fault. 1074 NEW YORK STATE MUSEUM South of this fault, the structure becomes more complicated. The eastern sharper and more closely crowded folds now appear, and with them a number of thrust as well as gravity faults. The structure of this area, as far as section 20, is shown on a larger scale on the section map, and will now be described _ in detail. | ; Just south of the point where Claverack creek strikes the eastern road, i. e. at fault no. 9, we meet with one of the numer- ous, more or less overgrown wood roads which lead up the mountain. Following this road, which leads off westward from the main road, we find, on turning at a bend, that we are follow- ing a depression along the strike of the strata. This depression _ marks the location of fault no. 10, a strike fault. To the west of this fault the strata dip 20° to 25° westward, while on the other side they dip as much or more to the east. The strike of the Manlius and the overlying Coeymans, east of the wood road, is at first nearly east and west, the dip being as high as 30° or 35° to the south. This is caused by fault no. 11, a short diagonal fault between 10 and 12. Between this shorter fault and the main strike fault (no. 10) a triangular surfaced block has been tilted to the degree indicated by the dip. As this block stands now, only the Coeymans and Manlius compose it. East of fault 11 the strata dip steeply to the southeast, the angle ranging from 50° to 75°, while the strike is n. 30° e. Nearly the entire thickness of the Coeymans is exposed three times in the region of these faults, as shown by section no. 7. The Manlius forms the eastern portion of the section, dipping, as far as exposed, about 60° to the southeast, thus showing a complete overturn of the strata, the Manlius resting on the Coeymans. . South of the triangular fault block the structure is somewhat simpler, being affected only by two longitudinal strike faults. The first (no. 10) brings the steeply eastward dipping New Scotland (70°, s. 60° e.) against the gently inclined westward dipping Coeymans (20°, n. 60° w.), as shown in sections 8, 9 and 10. To the west of the fault the beds from the Coeymans up are shown, while on the east of this fault, the New Scotland, Coeymans and Manlius are found in the reverse order, owing — REPORT OF THE STATE PALEONTOLOGIST 1902 1075 to the overturning of the beds. A second longitudinal or strike fault (no. 12) begins in the Manlius on the northeast and a little later passes into the Coeymans [section 10] ending finally in a small diagonal fault. Thus once more eastward dipping beds are brought in contact with the steeply overturned strata, par- tially repeating the Manlius in the upper, and the Coeymans in the lower section (nos. 9 and 10). A little farther southward, another triangular fault block occurs, bounded by faults 11, 18 and 14. The probable struc- ture of this block is shown in section 10. On the east the over- turned Manlius, Coeymans, New Scotland and Becraft are visi- ble, all dipping very steeply to the southeast, some beds being almost or quite vertical. A low ridge of Becraft with the strata standing vertically, is succeeded westward by a flat valley [see section 11] in which no strata are exposed. This valley is bounded on the west by fault 10, beyond which is another ridge, on the summit of which the Becraft is again seen dipping 40° northwestward. No exposures are shown at the base of the ridge at this point, but it is almost certain that the New Scot- land lies at its base and that it is merely a southward con- tinuation of the same structural ridge found just northward, where the New Scotland is shown. The westward dipping Strata are bounded on the east by fault 10, which has here turned more to the west. What strata occur between the fault and the low ridge of Becraft have not been ascertained, as no satisfactory exposures were noticed. Some rock masses which appeared to be in place, were finely crystalline, shattered and veined limestones, which may represent either the Coeymans or Port Ewen. No fossils were obtained, but from the character of the strata a little farther south [section 14], it appears most natural that the valley is occupied by a closed synclinal fold of Port Ewen, with possibly some Oriskany in the axis of the fold (which would account for the valley). The Becraft probably comes up again on the other side of the syncline, next to the fault. Fault 14 is followed by an old wood road, which leads down to the main road east of the mountain. South of this fault the Manlius forms the greater part of the surface. It 1076 NEW YORK STATE MUSEUM forms a synclinal trough, the axis of which dips 10° southward. The appearance of this portion of the surface is therefore some- thing like half of a shallow basin. On the western side of the trough the rocks are sharply overturned, so that they dip &/° to the eastward, but with their uppermost side down. This overturn fold bounds a flat bottomed tract or longitudinal val-. ley. On tracing the fold southwestward along the strike, it is found that less and less of the upper Manlius strata are uncov- ered in the axis of the fold; and that, finally, they are covered en- tirely by the Coeymans limestone. This again shows the south- ward pitch of the fold. As shown by the eastern ends cf sections 14 and 15, the strata there are involved in another simple anti- clinal fold (no. 4), which, from the southward pitch, is formed on the present surface by progressively higher and higher strata in that direction. The western boundary of the aforementioned longitudinal, flat bottomed depression [section 14] is formed by a double ridge of Becraft, the eastern portion of which dips 60° eastward, while in the western ridge the dips are 25° to 30° to the west. A little farther south [in section 15] only the west- ward dipping ridges of Becraft, capped by Port Ewen and under- lain by New Scotland, occur. This shows that a fault line passes between the two sections. This fault is well marked to the southeastward, where the Manlius is thrust over the Coeymans. This overthrust fault is finely shown in the cliff facing the road- way along the eastern border of the mountain. Here the rela- tions shown in the following diagram are clearly exhibited. This overthrust fault appears to be earlier than, or at least contemporaneous with, the longitudinal strike faults (10 and 12), for the latter are not seen south of the overthrust fault. This fault may be traced northwestward as far as the little brook which drains the great meadow. Here it appears to pass into a strike fault and is not traceable any farther. As we go south- ward, the pitching axis of the fold reveals another fold as shown by the sections [15-20]. These folds are of the typical Appala- chian type, with a steep, overturned limb on the west and a gentler, normal limb on the east. Eastward this eastern limb again passes under and rises as the steep or overturned western \ REPORT OF THE STATE PALEONTOLOGIST 1902 LOTT limb of a second anticline. That this was another similar fold to the one discussed appears on comparing sections 14-20. It is highly probable that the western end of section 15, from the axis of the overturn fold now shown in the Coeymans near the middle of the section [A], was of the type of those of section 20. Zo TOS a ee === |, IEEE ETT ea OES toy Fig.13 Overthrust fault with infolded Manlius (a) and Coeymans (b) If the latter section were added to the eastern half of section 15, so that the extreme eastern end of 20 [A] coincided with the axis of the overturn anticline [A, section 15] we would restore what appears to have been the normal type of folding of this region. Beginning on the east, there was a simple anticline with the limbs nearly equal. This was followed by a broad syncline, with a gentle westward dipping limb on the east and a more abruptly eastward dipping western limb. The latter _ formed the eastern limb of the overturned anticline, which had almost become an isocline. The strata came up again in a broad syncline with overturned eastern and low western limb, after which they were again involved in an overturn anticline of the same type as the preceding. A similar syncline to the last fol- lowed, and was in turn succeeded by a third overturned anti- cline in the Onondaga, as shown in section 21. The syncline following this is of the same type as the two preceding; its western limb, with an angle of 12° or 15° eastward dip, forms the western side of Becraft mountain. We may safely assume that three close overturned anticlines existed, besides the appar- ently uniform anticline on the extreme east. The overthrust fault no. 15, the direction of thrust of which was from the south- west, produced a northward as well as eastward displacement A/F LA 1078 NEW YORK STATE MUSEUM of the strata from the southwest, thus bringing the axis of anticline 3 southwest of the overthrust [A, section 20] some 400 feet farther northeastward than its continuation north of this fault [A, section 15]. By this overthrust the western limb of syncline 3 [B, section 14, which corresponds to B, section 20] steepened from 380° to 60°, making this syncline nearly a closed — fold. Dee Going southwestward from section 20, the axes of the folds continue to pitch downward, so that higher and higher strata come to form the surface. This is well shown by a comparison of sections 20 and 21 and by reference to the map. We pass from the New Scotland beds, which in section 20 form the pres- . ent top of syncline 3 and anticline 2, to the Becraft and later on to the Port Ewen, only the steep eastern limb of syncline 3 remaining as a narrow band for each of the lower formations. The descent continues to fault 17, where an oblique shifting of all the strata occurs. Thus, as shown in section 22, the over- turned western limb of anticline 3 (the only portion of that anticline remaining) is repeated, the repeated portion however being more strongly overturned. From this fault the axes of the folds rise southward, lower and lower members being pro- gressively uncovered in the eroded anticlines. This is seen on comparing sections 22 and 23, the position of the latter with reference to the former being indicated by the dotted line in the lower portion of section 22. On comparing anticline 23 of sec- tions 22 to 25, this same southwestward rise or northeastward pitch of the folds is shown. It is thus apparent that on oppo- site sides of fault 17 the folds pitch toward each other, and it is noteworthy that at this, the lowest point of the strata, the stream which has its valley wholly on the Oriskany outcrops, breaks across the strata to join Claverack creek. It is at this point that the axis of anticline 2 is so low that the hard lime- stones are carried below the present level of the stream on the Oriskany outcrop, thus making this the natural point of exit. A comparison of sections shows, that the folds steepen toward the northeast and also become more closely crowded. Hence the lines marking the anticlinal and synclinal axes are closest EE a = i a ee ee a a re REPORT OF THE STATE PALEONTOLOGIST 1902 1079 together in this portion of the map. The pitch of the folds is well shown by the outcrop of the Port Ewen and Oriskany of anticline 1 and syncline 1 and 2. The adjustment of the stream to the Oriskany outcrop, or more specially to the con- tact between the Oriskany and Esopus, is well shown [compare section 24]. Fault 18 cuts off these folds abruptly and, to- gether with fault 19, which is its continuation, bounds this area. West of these faults, we have a strongly eastward pitching, sim- ple syncline, with gentle northern and vertical southern limb. This is a section of syncline no. 1, which, from representing the upthrow side of the fault is alone found, all the more southern folds having been worn away [sce section 26]. To the north of this syncline is a steeply eastward pitching anticline, which is apparently unrepresented in the other por- tions of the mountain. This fold is broken in the center, and a long narrow block, bounded by faults 20 and 21, has dropped down. Where these two faults converge, is a large, flat bot- tomed meadow, inclosed on all sides except the southwest, by steep banks which rise in places to a hight of a hundred feet or more. The meadow is drained through the open end by a west- ward flowing stream. | The sides of this depression are so steep and fresh and the bottom so flat, as to suggest some recent movement along the bounding fault planes. The inclosure on the three sides is so abrupt, as to make any other explanation difficult. Moreover, the bottom of the depression is underlain by the New Scotland beds, the same which form the sides of the hollow, and there is no assignable reason why one part should be so maturely eroded while the adjoining portion is still so fresh. It is not improb- able that this impression represents a sink hole of unusual dimensions for this portion of the country. The approximate dimensions of the depression at the bottom are: length 650 feet; greatest width 300 feet [see section 26]. Beyond fault 21 to the northern extremity of the mountain, the structure is very simple and uniform, as shown by section 1. A NEW EURYPTERID FAUNA FROM THE BASE OF THE SALINA OF WESTERN NEW YORK! BY CLIFTON J. SARLE With 21 plates INTRODUCTION In western New York the outcrops of the Salina strata occur in a belt of country averaging 10 miles in breadth, parallel to the southern shore of Lake Ontario, and its northern limit dis- tant thence about 15 miles. On the Rochester meridian the for- mation is 600 or 700 feet thick, and, in the lower portion, com- prises variously colored shales or marlites, interspersed with some thin layers of dolomite, while in the upper portion are salt and . gypsum deposits with some beds of waterlime and limestone. The exposures of the formation in this part of the State are few, owing to the very destructible nature of the rock and to a heavy covering of drift. No sedimentary strata in the State have been considered more barren of fossils. Resting on the Lockport dolomite, which is everywhere replete with fossils, and underlying the Bertie waterlime, which at many locali- ties carries a rich assemblage of eurypterid remains in the thin layers at the top, it has formed a conspicuous break in the paleontologic record. It is therefore a-matter of considerable interest to announce a rich eurypterid fauna, discovered by the writer in 1898, in the basal layers of the Salina formation, in Monroe county. This fauna, though separated from that above by nearly the whole thickness of the Salina, is its counterpart in many respects but perhaps more primitive in its characteristics. The discovery thus affords additional ground in support of the com- — prehension within the Salina of all beds included between these faunas. Formerly this association was based entirely on stratigraphic succession and a supposed similarity of physical conditions, from which it was assumed that a similarity of life must be found. 7 It is safe to state that this is the earliest fauna yet known to which the name “eurypterid fauna” can be properly ap- *Since this paper was put in type it has been accepted by the faculty of the University of Rochester as a thesis for the degree of master of science. ; ; : : REPORT OF THE STATE PALEONTOLOGIST 1902 1081 plied. The remains from earlier formations are extremely rare and, almost without exception, very fragmentary. Euryp- terus boylei Whiteaves (1)! was described from a single nearly complete body found in the Guelph dolomites underlying the Salina in Ontario; Eurypterus prominens Hall (2), from a cephalothorax referred on doubtful grounds to the Clinton of Cayuga county, N. Y.; fragments of Pterygotus were described by Barrande (3) from the Siluric of Bohemia; the genus Echinognathus Walcott (4) was described from a single limb found in the Utica shale (Lower Siluric) of New York; Eurypterina Walcott (5), from fragmentary remains found in the Belt terrane (Precambric) of Montana; and recently, the genus Strabops Beecher (6), from an essentially entire body _ found in the Cambric of Missouri. Other forms of life occur with the eurypterids in this fauna, but they are comparatively inconspicuous and have no effect on the general facies. The entire fauna comprises: Graptolitida 1 Ostracoda 1 Annelida (denticles) 3 Phyllocarida 2 Brachiopoda 1 Synxiphosura 1 Pelecypoda 1 Eurypterida 6 Cephalopoda 2 — Total 18 Three species from the original collection made by the writer, have already been described by Dr John M. Clarke (7), viz, two phyllocarids representing the genera Ceratiocaris (C. prae- cedens) and Emmelezoe (E. decora), and a merostome belonging to the synxiphosuran genus Pseudoniscus (P. roosevelti). Five new species of eurypterids and a variety of one of these are here recognized, representing four genera, one of these being new to science. The specimens re- ferred to four of the species are so fragmentary that at present they do not warrant complete determination, it being preferable to wait till more perfect examples have been obtained. These fragments, however, have been figured and will be referred to briefly. a See references on p. 1109. 1082 NEW YORK STATE MUSEUM The collection was obtained from excavations made in deepen- ing the Erie canal during the winter of 1897-98. The precise locality begins at'a point a few rods east of the Brighton- - Pittsford line in the latter township and extends southeast for a distance of about 300 yards. Though the exposure did not at any one point exceed 9 feet in hight, yet, owing to the dip of the strata toward the east, higher levels were brought down to view, so that the entire vertical section was about 16 feet. ~The rock is a soft shaly marlite, in layers of different colors, often mottled, and interspersed with a few thin layers of very hard, fine grained dolomite. The eurypterids are found in a rather fissile, very dark olive- green to black shale, which, like the adjacent argillaceous strata, rapidly disintegrates on exposure. The beds of this section in descending order are: Feet Inches in reed: Slraler. 20S Pr aaneae os axle ae a ete reenter Sapient 6 2 Light gray, compact, fine grained, dolomite, with. imperfect conchoidal fracture, weathering 3 hight brown to eream .Coloryt.4. 400 <7. 10 3 Soft, gritty mud-rock, purple with bright red mot- LBA 0 24 Sener ater AL genre AE ENS SA Ace wi ee ae By 4° Dolonmte Wke m0: 2. ou sais ose ean a eens eres emer 4 5 Purple shale with red mottlings............... 1 1 6“ Green-shale rr Mii Pell ties mete hens Secuencia i’ 2 7 Thin layer dolomite like no, 2:2... 5. wee | 4 8 Black shale, very compact, the base splitting un- evenly; grading to olive-green shale in the WP POR ADA ee ee wake cies oe rere se ene nes 10 9 Dolomite likes woe Qe ee vee ee ac ae. chee nes ee Beige) 10 Black shale, with leaf of dolomite 14 inch thick four inches from its base..... peak once: Oa ak 2 11s Dolomite like n0. 27.055 Seo EAS eee: ue” 12 Soft, green, arenaceous mud-rock, occasionally be- coming shaly; the lowest exposed rock of the . Gi | Gea Pao ei DER aa yim Aine MAN tu! ol le bial & f ian The shiyaterta fauna occurs in the black aiale nos. 8 and 10 in the foregoing table. REPORT OF THE STATE PALEONTOLOGIST 1902 1083 The proximity of this cut to wells penetrating to the Lockport dolomite, and to exposures on the west branch of Allen creek within half a mile to the north, show that the section is located on the northern edge of the Salina formation, hence approxi- mately at its base. The accompanying table, representing the beds lying between the black shale and the Lockport dolomite, as well as those for some distance above, was made from an examination of well sections a little to the westward of the fossil locality, and from a series of outcrops along the creek. The level of the black shale is thus ascertained to be about 20 feet from the base. From wells: Sale Sige a ee Sven ge HALe GY. MATIC ..5 ese 5 6 o ose tle eh eb os ore epee ee 10 2 Hard, fine grained, yellowish, dolomite, having an imperfect conchoidal fracture............ 2 MIR eet tas ee gl ne eran Si, eee heart ns 1 mei RUMEN PITMNALCG Gb fe. 3. 5 Ze kbensid os aid oad vc oviae ook a PMIIBIENBE ITO TOD). ocsc0k v2. cok velco ee.g bie awk 5; a oo ™ o = a9 Cay - © 5. Ne oO: a ae Op hc oe Omer crf 2 om «¢ b> (ee) BPM MSA, of waid 2 = tio Sis cial ® «pita 4 bia'ets «mits wr 2 4) 10 Black shale, very fine textured, fissile, and with 1 inch dolomite parting (eurypterid horizon).. 1 6 emer HITE Fae 8 sakes, 3245, ac iv acd’ Give 9-5! « tesa e 1 momeemiinie like N10. 2.6... od one ceive ov cncceee 2 eerrertnshale OF Marlite. .. . 6. sc. us osc cece owsec 6 From west branch of Allen creek: 14 Light colored waterlime, some pyrites and sun TEE EIS Sy SS Oe RIG tee Pa eS a 5 iimeeees-oreen shaly marlite ......5..0002 600 esse ese ¢ ail r Niagaran 16 An impure yellowish porous limestone 17 Succeeded by an impure bituminous limestone made up of imbricating, shell-like domes ete. 1084 NEW YORK STATE MUSEUM The portion of this section which corresponds to that in the canal cut, is seen to show some differences. However, the rapid changes in character of the Superposed beds may be taken as a good indication of the limited lateral extent of most of them. The red shale appearing in the upper part of this sec- tion is the same as that exposed in the upper part of the canal cut. At Pittsford, 2 miles southeast of this cut, the canal is excavated through red shale mottled with green. At Carters- ville, 2 miles farther southeast, this same rock occurs in the canal bed and 40 feet lower in the waste weir. At Fairport, 4 miles northeast of this, it is again exposed in the canal, and by well-borings is shown to have a considerable thickness at that place. It thus appears that this red shale corresponds to the lowest division of the Salina recognized in western New York by Hall, and immediately overlies the stratum containing the fauna herein described. | | A few important facts relative to the physical changes attend- ing the introduction of the Salina fauna into the area are well illustrated by these sections. The exposures on the west branch of Allen creek, from which the lower part of this sec- tion was taken, show in the upper portion a progressive change of conditions: first, from those of the Niagara sea, in which stromatoporid reefs were widespread and an incipient Guelph fauna flourished, to those under which thin layered, impure, ripple-marked dolomite was deposited and fucoids appear to have been the only forms that abounded; then, to conditions for the formation of a tough, porous, very bituminous lime- stone, succeeded by a phase during which a stratum of thin- layered, bituminous accretionary limestone, forming flat, imbri- cating, shell-like domes,! was deposited; and, finally, to condi- 'This rock is the same as that south of Lockport, Niagara co. noted by Hall, Geol. N. Y. 4h Dist. p.92, "and also exposed in the southern part of the city of Niagara Falls. It is probably identical with that described by Vanuxem in the Geol. N. Y. 3d Dist. p. 91, as a limestone, small in quantity and in hem- ispheric concretions, whose parts are more or less concentric to each other like the coats of an onion, and regarded by him as an attenuation of the Lockport dolomite. | REPORT OF THE STATE PALEONTOLOGIST 1902 1085 tions during which 2 feet of light yellowish impure limestone, showing on the weathered surface casts of a very finely branch- ing organism, probably a plant, were formed. On this rests a - greenish shaly marlite, the basal stratum of the Salina. The next layer consists of a bench of waterlime marked by shrink- age cracks, indicating a temporary exposure to the air during the time of formation. It is thus seen that preparatory, as it were, to the coming of the Salina fauna, there was a marked change in physical conditions. The shallowing of the sea, with a probable increase of salinity and turbidity of the waters, probably had more than anything else to do with the displacing of the Niagara fauna. While these changes were going on, the first of the Salina fauna, a Pterinea, a little more rhomboid and convex than P. emacerata of the Rochester shale, appeared. Later, in the waterlime bench, besides the Pterinea, a Lingula, a Leperditia (L. scalaris), and also an Orthoceras, occur. With the exception of the last, which has not been noted else- where in this section, these fossils make their next appearance in the black shale, where they are accompanied by the eurypterids. z The eurypterids are by no means uniformly distributed throughout this shale. The species representing the new genus to be described, occurs most abundantly in the lower half, where it is so prolific that certain planes are literally packed with its remains, making this probably the richest eurypterid stratum known. The genus Eurypterus, represented by a single large species, occurs most frequently in the upper half of this black shale, just above the 2 inch limestone parting. The Ptery- gotus head [pl. 24, fig. 7] was also found in the upper portion. The dolomite layers associated with this black shale are marked by an almost complete absence of eurypterids, the Leperditia and Pterinea, with the exception of an occasional specimen of a small pentalabiate Gomphoceras of character- istic Siluric type, being the only forms found in them. From the fact that the occupation of the area by the merostome fauna followed one of these dolomite-forming intervals, was twice 1086 NEW YORK STATE MUSEUM interrupted by the accumulation of marl, and finally was closed by another lime-forming interval, it is evident that the condi- tions at these times were not favorable to the eurypterids. These dolomitic limestones probably represent more open water, or the temporary removal of some barlike barrier, and, probably, | a diminution in the salinity of the water. Though the fine char- acter of the silt forming the black shale and the evidence of interrupted sedimentation noted above, indicate slow accumula- tion, the occupation by the eurypterids was apparently of comparatively short duration, merely an incursion, as it were, since the black shale all told does not exceed 2 feet in thickness. The fact that the eurypterids are often dismembered and their parts distributed over considerable areas, and that a dozen or more are frequently found side by side, with a com- mon flexure, suggests that they may have been drifted up by a current. On the other hand, the fine preservation of much of the material, extending even to the delicate appendages, shows that the currents were very weak, thus practically leav- ing the animals in the position of death or molting. Their grouping is very probably due also, in some degree, to their gregarious habits or to their abundance. The tests. of the eurypterids are black and carbonized. A line of dehiscence around the anterior edge of the cephalothorax indicates that in many cases these remains are moltings. REPORT OF THE STATE PALEONTOLOGIST 1902 1087 DISCUSSION OF SPECIES Genus HUGHMILLERIA gen. Nov. - By far the most abundant of the eurypterids occurring in this stratum of black shale near the base of the Salina, is a small form which, from its general appearance, in many ways suggests the genus Eurypterus, while a study of its structure shows it to be closely related to Pterygotus. It is evidently a new genus, which it is proposed to designate by the name Hughmilleria. Generic Magnosis General outline lanceolate. -Cephalothorax semielliptic and flatly convex; compound eyes small, subelliptic and marginal; ocelli subcentral. Abdomen divided into distinct anterior and posterior regions. Preabdomen provided dorsally with six plain, transverse, bandlike tergites; ventrally with five stern- ites, the last three being essentially like the corresponding dor- sal plates. First sternite cleft for the reception of a median appendage, which varies in form according to sex. Basing sexual distinctions on the determinations made by Holm in EKurypterus fischeri, this appendage in the female _cousists of a narrow, convex, scalelike, sagittate-based sheath, which appears to be formed by the fusion of two nearly equal portions, the anterior overlapping, and projecting poster- ‘iorly to cover partially a slightly shorter, simple, lance-linear ap- pendage in a cleft of the following sternite. In the male the appendage is confined to the first sternite, the second being en- tire. It is proportionately shorter and broader, convex and lanceolate with the posterior free end slightly produced. Post- abdomen composed of six ring segments. The first is readily distinguished from the segments of the preabdomen by post- lateral prolongations. It appears to be formed by the fusion at their appressed ends, of a sternal and a tergal portion, the latter of which is the longer. The following segments are sim- ple, bandlike rings. Telson long, lanceolate, with dorsal carina- tion. Epistoma convex, peltiform, dividing in molting or under Stress of compression, through the middle, joined at the sides to a narrow doublure. Preoral appendages attached at the pos- 1088 NEW YORK STATE MUSEUM terior end of the epistoma; short, stout, composed of three joints, the two distal a little shorter than the basal, and forming a pair of edentulous, bevel-edged pincers, which normally are folded back so that their tips converge close to the anterior end of the mouth. Endognathites increasing in length from the first back- ward, moderately robust, spiniform, composed of seven joints, of which the third to the sixth inclusive bear a pair of spines. Swimming arms narrow, lanceolate paddles, composed of eight joints and a rudimentary ninth inserted in a notch on the inner side of the eighth or palette. The proximal joint, or gnathobase, has the form of an upright retort. The seventh bears on the inner half of the distal end a subtriangular lobe demarked by a suture. Metastoma elongate, cordate. Type, Ji... S0-¢la las Sazrle. Comparison with other genera The characters suggesting Pterygotus are: the rounded tri- angular or semielliptic outline of the head as seen in Pt. banksii Salter (8) and Pt. raniceps Salter (8); the marginal, compound eyes; the slender body with slight constric- tion between the anterior and posterior abdominal portions; the cordate form of the metastoma; and the simplicity of the opercu- lar plate and its appendage. The two forms of this append- age resemble those of Pterygotus as far as the material — of the latter permits of comparison, one form being a slender, sagittate-based scale, the other a shorter, broader, convex body, asin Pt. bilobus Salter (11) and Pt. osborni Hall (10). In the new genus the first form projects posteriorly to _ protect a shorter lance-linear appendage lying in a cleft of the second sternite, while the second form is followed by an entire sternite without appendage. The sixth pair of cephalothoracic appendages resemble those of Pterygotus in being only shghtly expanded distally and consisting of eight joints, with a rudi- mentary ninth inserted in the end of the palette. The gnatho- bases have the upright retort form. This genus is distinguished most clearly from Pterygotus by | the character of the preoral appendages. These are stout, three- REPORT OF THE STATE PALEONTOLOGIST 1902 1089 jointed, chelate organs, so short that when extended they barely equal one half the length of the cephalothoracic shield. The _ pincers are edentulous and bevel-edged and in their normal posi- tion lie folded over the basal joints so that their tips converge _ close to the anterior border of the mouth. Extended, these © organs project beyond the border of the shield for perhaps half their length; when turned straight back, their tips lap over the end of the metastoma. In Pterygotus, on the contrary, these organs are very long, having, at least in Pt. bilobus Salter and Pt. macrophthalmus Hall, a length fully one third that of the entire animal; and consist of ponderous, dentate pincers supported on a slender, retrally tapering proxi- mal joint of such a length as must necessarily have prevented _ the pincers being used at the mouth, unless these appendages were somewhat retractile, as suggested by Laurie (9). The next important difference is in the character of the spini- form walking legs. As in Pterygotus, these consist of seven joints, but the several pairs present a greater contrast in their respective lengths, are proportionally more robust, and each joint from the third to the sixth inclusive, carries a pair of ven- trally and distally articulated, slender, curved spines. It is doubtful if any species of Pterygotus has spines on these ap- pendages; certainly, in several species in which these limbs have been found apparently well preserved, they are lacking. Woodward (8) represents Pt. taurinus Salter as having a spiniferous endognathite. Laurie, in his Anatomy and Rela- tions of the Ewrypteridae (9), in one place states that there is no elaborate development of spines on the endognathites of Pterygotus. Earlier in the same paper, however, he makes the statement that they are destitute of anything in the way of spines and, in a comparison of the appendages of Slimonia with those of this genus, offers this explanation: “These [dentate, preoral] appendages, unlike those of Slimonia, were probably prehensile rather than masticatory, and this function may account for the absence of spines on the other limbs (en- dognathites), which are purely ambulatory.” The converse of this may be stated of Slimonia, and also of Hughmilleria, since 1090 NEW YORK STATE MUSEUM the pincers are edentate and the walking limbs carry light, claw- like spines. The epistoma, instead of parting on either side from the doublure by stress of compression or in molting, as an epistoma of Pterygotus figured by Laurie (9) did, is seen to have divided through the center, an occurrence observed in a large number of specimens. Schmidt (12) figures an epistoma of Pt. osil- iensis Schmidt, which, while showing a tendency to divide along sutures at the sides, has also a deep open cleft in the posterior edge. It is evident that there is considerable varia- tion in this plate in different species. The last of the differences lies in the telson, which is slen- derly lanceolate and much longer than that of any known species of Pterygotus. Regarding its resemblance to Eurypterus, it might be said that, but for the marginal position of the eyes and relatively large chelae, this form would easily be mistaken for a species of that genus. The semielliptic form of the head and the slight expansion of the swimming arms, recall E. lane eolatus Salter (8), and.the slender telson gives the posterior part of the body of a general Eurypteruslike appearance, hightened by the spiniferous character of the walking legs and the short, edentulous, masticatory preoral appendages. However, the walking legs are less robust. They consist uni- formly of seven joints and are equally spiniferous, while in Eurypterus, with the exception of.the first pair, there are more than seven, and the fourth pair carries merely the three end spines. In the preoral appendages, the basal joints, instead of being flat expansions on which the pincers are articulated (15), are segments a little longer than the pincers, which, in their normal position, instead of hanging down over the mouth, do not quite reach its anterior end. These pincers have been seen in Eurypterus only in the Russian species E. fischeri. The limbs of the sixth pair are less expanded at the ends than is usual in Eurypterus, and have narrow, upright, instead of heavy, subquadrate gnathobases. The operculum is simpler, lacking the faint transverse suture and two subtriangular REPORT OF THE STATE PALEONTOLOGIST 1902 1091 areas which in the female Eurypterus le in front, one on either side of the median suture. The parts of the genital appendages correspond in a general way to those of Kurypterus, though there is considerable difference in their form. In the female the appendage consists of two parts, one carried by the operculum, the other by the following sternite. The part car- ried by the operculum is slender with a sagittate base, and is divided transversely into two portions, but lacks the pair of short, flat, diverging, terminal crura. That carried by the sec- ond sternite is simple, broader at the base and attenuated at the distal end, instead of having articulated to it, two diverging, ensiform strips (14). In the male, as in Eurypterus, the ap- pendage is confined to the operculum, and is shorter and broader than that of the female; but is proportionately larger than in that genus. The genus Slimonia is suggested in three ways: by the mar- ginal position of the compound eyes, by the shortness and edentulous character of the masticatory preoral appendages, which are, however, less robust in that genus, and by the length of the telson and the slight indication of inflation in the an- terior portion. In other respects there appears to be consider- able difference between these genera. From a consideration of the foregoing facts, it appears that Hughmilleria is most closely related to Pterygotus. With Pterygotus and Slimonia, it makes three genera of eurypterids having the compound eyes marginal. In development of preoral appendages, it comes between Pterygotus and the other genera in which these appendages are known, including Kurypterus, Dolichopterus, Stylonurus, Eusarcus and Slimonia. Hughmilleria socialis sp. nov. Plates 6-9; 10, fig. 1-6, 8-9; 11-14; 15, fig. 4-6; 24, fig. 1; 25, fig. 1 ,8, 4; 26, fig. 3, 5 This type is comparatively small, the length of the average individual not exceeding 15 cm. Viewed from either the dorsal or the ventral side, the outline is slenderly lanceolate. In the natural, undistorted condition, the anterior part of the body is flattened, the dorsal and ventral surfaces being slightly con- vex, while the caudal portion is nearly cylindric. 1092 NEW YORK STATE MUSEUM Cephalothorax. The cephalothorax is semielliptic or subtri- angular in outline, the length equaling the breadth at the base, and comprising about one fifth the length of the entire body. Along the gently curving sides and acutely rounded front is a narrow flattened border, striated on the under surface, and not exceeding a fraction of a millimeter in breadth. The dorsal sur- face is slightly rounded or arched from the side to the center, so that in an undistorted shield 22 mm long, the elevation is about 2mm. The posterior edge, except for a slight forward curve at the genal angles, is straight. The compound eyes barely break the outline of the shield; they are small, elongate, widest anterior to the middle, the outer side arcuate, the inner formed by three nearly straight edges—a short basal and a little longer anterior, forming slightly rounded obtuse angles with a long inner side. The anterior end of the eye is acute. The length of these organs on the cephalothorax, the dimensions of which were given ( above, is 5 mm. However, the usual proportion between the length of the shield and eye is as 1:4.5. A line drawn connect- ing the posterior ends of the eyes passes through the center of the shield. The ocelli are situated on a small tumescence cut by this line; they form two minute, ringlike prominences sepa- rated by about the length of their diameter. ; Abdomen. The abdomen, at the widest point, or between the third and fourth dorsal segments, is a little wider than the base of the cephalothorax. Thus, in one animal measured, these dimen- sions were respectively 24 mm and 17.5 mm, in a second 23 mm and 17 mm, and in a third 33 mm and 26 mm, probably varying somewhat according to the amount of compression and also somewhat with. the animal. From this point the abdomen tapers very gradually to the telson; it is divided into anterior and posterior parts, easily distinguished by their structure. The preabdomen consists of six dorsal and five ventral, trans- verse plates; the postabdomen of six annulate segments and one spiniform. Preabdomen. The first tergal plate of the preabdomen is very narrow and is overlapped by the posterior margin of the shield. Its posterior edge is slightly convex, and its ends are rounded. REPORT OF THE STATE PALEONTOLOGIST 1902 1093: ( The second segment is twice as long as the first, its posterior edge is slightly concave along the middle portion, and the posterior angles are rounded, while the anterior are produced, to make up, as it were, for the rounding away of the preceding tergite. The succeeding tergites are very nearly equal in length, the fifth being perhaps a little the longest, and are about one third longer than the second. The posterior margins are concave as in the preceding, but straighter near the sides,. forming almost right angles. The first ventral plate, or sternite (the operculum), is- one third as long as broad, and is divided along the axial _ line into two equal parts. These are rounded off at the lateral angles, particularly the anterior, and excavated along the median line for the reception of the opercular appendage; the posterior edges are slightly projected on either side of this, while the anterior inner angles are projected forward, forming a com- pound median lobe. The second sternite, in the female, is nearly as long as the operculum, and is deeply cleft for the reception of an appendage nearly equal to it in length. The sides are cut obliquely forward, making the posterior angles rather acute; the anterior angle forms small lobes, and the middle of the anterior edge is slightly produced. In the male the last four sternites, and in the female the last three, do not differ mate- rially from the last four and three abdominal tergites. The relative position of the several plates of the sternal series to- those of the tergal, is as follows: the opercular plate begins a little farther forward than the first tergite, but, owing to its. greater breadth, lies beneath the line of overlap of the first and second tergites, while the second sternite lies beneath the over-. lap of the second and third tergites, and so on, the last sternite. underlying the overlap of the fifth and sixth tergites, thus not extending as far back as the posterior edge of the sixth tergite. Postabdomen. The first postabdominal segment consists of a tergal and a sternal portion united by their appressed: pleural ends. The postlateral angles are prolonged into short, bladelike lobes which extend alongside the following segment for fully half its length. The tergal portion is the longer, ~ 1094 NEW YORK STATE MUSEUM and its posterior edge forms a broad lobe; the sternal portion is Short, and its posterior edge is straight, while its anterior edge extends forward to meet the last sternite of the preab- domen. The following five segments are plain, bandlike rings, decreasing in breadth backward. In the first the breadth is considerably greater than the length; in the last, or penultimate body segment the length and breadth, in compressed specimens, are equal. The anterior end of each of these segments is marked by a groove for the attachment of the interarticular membrane. | | } The telson is very slenderly lanceolate, widest near the an- terior end and attenuated at the tip. In length it is equal to the four preceding segments. ‘The dorsal surface is convex, rising from sharp, lateral edges to a median longitudinal carina, which begins in the anterior part as a broad, angular promi- nence; the ventral surface is nearly flat or faintly convex; a cross section is thus subtriangular. Compression usually flattens the sides and thus hightens the angular appearance. The uncompressed specimen [pl. 15, fig. 6] has a length of ol mm and a greatest breadth of 7 mm. On the ventral surface of the cephalothorax, in front, is a convex lobe or platform, the epistoma, from which extends a flat, tapering doublure ending in a small expansion at the genal angles [pl. 11, fig. 6 and pl. 12, fig. 2]. In molting and also from compression, the epistoma divided through the middle rather than along the sides [pl. 12, fig. 2]. ) Appendages. The preoral appendages are short, stout, three jointed, chelate organs attached at the posterior border of the epistoma [pl. 11, fig. 7]. The two distal joints of each form a pair of broad based, edentulous, bevel-edge pincers, in the ordi- nary state of compression having a breadth equal to one half the length. The blades are about equal in length to the basal por- tion and meet at the very acute, slightly curved tips and again, usually, only near the base. There is considerable variation in the relative form of the pincers, as shown on plate 11. The broad basal joints are about one fourth longer than the pin- cers, widest near the base and longest on the inner side, and in REPORT OF THE STATE PALEONTOLOGIST 1902 1095 the natural position extend beyond the anterior margin of the shield for about one third their length. The pincers articulate with this joint in such a way that, when folded backward, they cross it obliquely, and their tips converge a little in front of the - mouth; when extended forward, they diverge somewhat. The preoral appendages could also be turned back to their full length over the mouth, the pincer tips then overlapping the metas- toma [pl. 11, fig. 6]. In an individual having a cephalothorax 22 mm long, the preoral appendages are 10 mm long. (Plate 9, figure 1, shows these organs from the dorsal view, the cephalo- thorax having been removed.) The four pairs of endognathites, or crawling legs, do not differ materially from one another except in length. The anterior limbs are somewhat shorter than the extended preoral ap- pendages, and their tips extend but very little beyond the margin of the shield. Each succeeding pair is about one half longer than the preceding, so that the last limbs are probably four times as long as the first. AJ] have seven joints, of which the terminal is spiniform. The third to the sixth joints inclusive carry ventrally and at the distal ends a pair of striated, slightly curved, slender spines. The inner spine of each pair is the longer, and the length increases for each successive set, from the third to the fifth joints; the spines on the sixth are short. The coxal joints are elongate, slightly curved, widest at the base and equal in length to the succeeding two joints. They increase in length with each successive pair, and bear on the inner end a series of 15 or more, sharp, curved teeth, which de- crease in size from the front. On each of the fourth coxal joints is a large perforation of the upper side near the fixed end [pl. 26, fig. 5]. No epicoxite has yet been observed. The second joint of the endognathite is divided by constrictions into three transverse sections. It is articulated at the fixed end of the coxal joint and is fully two thirds as wide. The limbs of the sixth pair are narrow and paddlelike, and con- sist of eight joints and a rudimentary ninth or claw, the seventh and eighth forming a slightly expanded blade. The seventh car- ries a large, subtriangular, lobelike plate, nearly one half as 1096 NEW YORK STATE MUSEUM long as the joint proper, marked off from the inner, distal end by a suture. The eighth, or palette, is elongate oval with the margin finely incised, and carries the minute claw inserted in a notch on the inner side near the tip. On the dorsal surface of the seventh and eighth joints, at the proximal end and outer edge of each, is a group of minute, craterlike tumescences, which were probably receptacles for the bases of hairlike bristles [pl. 14, fig. 8]. In a swimming arm 29.5 mm long, exclusive . of the gnathobase, the narrowest joint or the fourth, measures 9 mm across; from this point the arm gradually enlarges to 6.8 mm on the seventh and eighth joints. When the swimming. arms are turned back, they reach the line of the fourth or fifth dorsal segment. The gnathobases have the form of an upright retort. The inner extremity of each is provided with from 18 to 20 sharp, slightly curved teeth, which become finer posteri- orly. A gnathobase, accompanying a cephalothoracic shield 22 mm long, is 16 mm long; the width of the narrow necklike portion 6 mm; the width at the base 13 mm. The metastoma is elongate cordate, the greatest breadth com- ing anterior to the middle. The smaller, or posterior end, is truncated and has rounded corners. The anterior notch is rather deep and broad. A comparison of the length to the greatest breadth of several metastomas gives the proportion of 2:1. In an individual having a cephalothorax 23 mm long the metastoma is 16 mm long. ct The genital appendage differs noticeably in the two sexes. In the female it consists of two parts, one carried by the operculum, the other by the second sternite [pl. 13, fig. 1, 2]. The opercu- lar appendage is a slender, sagittate-based, convex, scalelike sheath projecting for about one fifth its length beyond the posterior edge of the operculum and appearing to be formed by the fusion of two parts. The anterior of these includes the sagittate base and a narrower, more convex portion with a flattened border on either side [pl. 18, fig. 4]. Its distal end is reentrant [pl. 24, fig. 1] and fused to the posterior part. This part is a little narrower, slightly tapering and beveled in from. - either side for one fourth the breadth, to the sides of a slightly raised platform which is flat topped for the greater part of its REPORT OF THE STATE PALEONTOLOGIST 1902 1097 length, but becomes concave posteriorly, forming a shallow groove at the abrupt end. The terminal angles are noticeably truncated. The appendage carried by the second sternite is par- tially covered by that of the operculum [pl. 14, fig. 2]. It is very slender, its greatest breadth not exceeding one sixth the length [pl. 26, fig. 3; 18, fig. 4]. The anterior half is sublanceolate with a triangular base; the posterior is attenuate and termi- nates just within the end of the cleft. In the male the ap- pendage is simpler and confined to the operculum, the follow- ing sternite being entire [pl. 18, fig. 3]. It is wider and some- what shorter than that of the female, the average length being only about two and one half times the breadth. It is convex, broadly lanceolate and slightly produced at the posterior free end which just clears the edge of the operculum. A specimen. _in which a portion of this organ is scaled away [pl. 14, fig. 1] gives a cast of the interior showing small elevated lines radiat- ing from near the center backward, and may possibly represent part of the vascular, or duct system of this organ. The two sexes are about equally represented in numbers. The whole surface of the body is covered with imbricating, crescentlike or angular scales, sometimes carrying smaller ones of the same pattern. These scales are so minute on certain areas as to appear almost obsolete. They are most con- spicuous on the ventral side of the preabdomen and appendages. ‘On the cephalothorax and abdomen the scales point backward, on the paired appendages toward the distal end, and on the epistoma, forward. Hughmilleria socialis var. robusta var. nov. Plate 21, fig. 1, 2 What appears to have been a varietal form of Hughmil- leria socialis is represented by a nearly entire abdomen, two first ring segments and an imperfect metastoma. The features which distinguish this form are: its larger size; proportionately much greater breadth; the greater convexity of the dorsal posterior edge of the first ring segment and, in Some cases, the division of this edge into two, broad, smooth lobes; the more noticeable contraction of the abdomen at the - 1098 NEW YORK STATE MUSEUM second ring segment; and the more rotund form of the metastoma. The abdomen found lies in the shale dorsal side up, showing the anterior nine segments well preserved. The second and third ring segments are partially disconnected. The breadth of the preabdomen at the widest point, or between the third and fourth segments, is 51mm, its length 56 mm, the breadth of | the first ring segment is 42 mm, of the second 30 mm. The dorsal posterior edge of the first ring segments is entire and very noticeably convex. In each of the isolated ring segments a broad, deep notch produces a bilobation of this edge. A line of pittings close to this edge shows this feature to be natural. The proportions of the more perfect of these segments are: ‘breadth 43 mm, length of the dorsal side 22 mm, length of the } ventral 11 mm, length of the postlateral lobes 8 mm. The metastoma associated with one of these segments is apparently of a smaller individual and lacks the anterior notched end. At the widest part it measures 14 mm and, from there to the posterior end, 14 mm. It was at first thought that the distinctive features of these specimens might be merely old age characters of H. sociali is, but larger individuals of that species seem to show the same relative proportions as the smaller. However, it is considered that the differences shown by the incomplete material of the collection are not, of themselves, sufficient to warrant the found- ing of a distinct species. Genus EuRYPTERUs DeKay. 1825 Eurypterus pittsfordensis sp. nov. Plate 10, fig. 7; 15, fig. 1-3; 16-23; 24, fig. 2-5; 25, fig. 2, 5, 6 This species is comparatively rare and is not represented in the collection by any entire individuals. There is however sufficient material to enable its main features to be correctly — determined. _ The entire animal is large and robust, and broadest at about the third segment. The cephalothorax is two thirds as long | as broad, eyes of medium size, appendages heavy. The pre- abdominal and postabdominal portions are not strongly differ- REPORT OF THE STATE PALEONTOLOGIST 1902 1099 entiated; the telson long, probably equal in length to the five preceding segments. The cephalothorax is broad, rounded in front, the sides curving out near the genal angles, and the base straight, or very gently curving over the middle portion, and extending a little forward near the sides. The margin is beveled in for a distance, in the average sized individual, not exceeding 2 mm in the widest part or in front, narrowing and fading out at the genal angles. The extreme edge is slightly upturned. The com- pound eyes are separated by one half the breadth of the shield, with their bases in line with its center. They are prominent, reniform, broader at the anterior ends, and one fifth as long as the shield. The ocelli are situated on a faint tumescence between the centers of the compound eyes. They are rather large and separated by about their own diameter. Near the basal edge of the shield is a pair of sharp, raised, triangular scales, one on either side of the axial line. In some cases there is a row of shallow, flat bottomed pits on the beveled margin. The abdomen increases slightly in breadth from the base of the cephalothorax to the third segment, then tapers to the telson, there being no apparent constriction between the pre- abdomen and postabdomen. Tbe tergites are comparatively short, the length averaging a little less than. one fifth the breadth. They are broadly concave along the middle of their posterior edges, and each carries, bordering this curve, four raised, triangular scales like the two on the posterior border of the cephalothorax and the middle two in line with them. The five sternites are medially cleft and marked by transverse sutures, which give to each the appearance of having been formed by the fusion of two plates. With the exception of the first or operculum, they have the anterolateral angles projected forward into small lobes. In the operculum these angles are noticeably rounded away, and the anterior edge is projected into a broad median lobe. In the female the second sternite has a similar lobe. The annulate segments, or sclerites, com- prising the postabdomen increase in length and decrease in breadth from the first, which is very broad and short, to the 1100 NEW YORK STATE MUSEUM last in which the length exceeds the width of the anterior or wider end. They are depressed and have faintly defined pleural areas or flattenings at the sides. Each is prolonged on either Side, at the posterior angle, into a short, striated spur, which grows longer with each succeeding segment, those on the last forming conspicuous pointed lobes. The first two segments each carry on the dorsal side four triangular scales like those of the preabdomen, the third, fourth and probably the fifth, each two, the last none. This segment has a shallow notch in the middle of the dorsal, posterior edge, marked on either side by a small denticle, succeeded toward the sides by very minute ones. The series of striations of the lobes continue up the sides of the segment to its articulation with the preceding. On the ventral portion of each ring segment is a shallow posterior emargination fringed with lobelike teeth. Extending forward from near either end is a curved rent, a pair sometimes almost inclosing an irregular, oval area. ‘The telson is very long, nearly equaling in length the rest of the postabdomen. Tor a short distance from the anterior end it contracts rapidly, then continues slender to the abruptly rounded point. The edges are sharp and, from near the anterior end, are marked by short, oblique incisions. The dorsal surface is smoothly convex, the ventral has a flat topped carina which begins near the proximal end and extends to the tip. On the carina is a double row of pits like those bordering the cephalothorax. | The doublure, at its dehiscence in the axial line, equals in width about one fourth the length of the cephalothoracic shield. From this point it narrows toward the genal angles. The preoral appendages have not been observed. The endog- nathites are robust and vary greatly in length, the first pair being barely long enough to reach the shield border, while the members of the third clear it by fully three fourths their length. _ The fourth pair is known only by a coxal joint and a basal por- tion consisting of three joints. The first legs consist of seven . joints; the second and third each, of eight. In the first three, each joint from the third to the penultimate is provided with REPORT OF THE STATE PALEONTOLOGIST 1902 1101 two long, curved, striated spines. The terminal joints are com- paratively long and clawlike. The coxal joints are large. The first three are short and broad, the length being a little less than two thirds the breadth. They have narrow, curved, postlateral prolongations equal in length to the second joint. The lower, inner angles are rounded and crenulated. The dentate faces at the inner, upper angles are on slight prolongations, which grow - longer with each succeeding coxa. All three begin with two or three isolated, anteriorly directed, lobelike teeth, followed by slender conic ones, which become finer toward the posterior end. The fourth coxal joint is comparatively long. The inner lower angle is gently rounded away, and the neck supporting the narrow dentate face, long. The teeth appear to be compara- tively few and coarse. The epicoxite of the third left coxa is shown on plate 16, figure 1. The swimming arms are stout and Daieiatels long, extend- ing back nearly to the fifth tergite, and consist of nine joints. The gnathobases are subquadrate and large, and are provided with seven or eight short, bevel-edged denticles, the two anter- ior being large and prominent. The length of the gnathobase [see pl. 15, fig. 1] was 33 mm, its breadth 30 mm, the length of the dentate face 8 mm. The middle joints have the anterior and posterior angles sharp, in the fifth the anterior forming a blunt, striated spine, much like those at the sides of the postabdomen. The seventh and eighth joints are broadly expanded, and their margins, particularly in the latter, are marked by sparse, shallow serrations. Inserted on the inner side and near the end of the eighth joint, is a small, oval, rudi- mentary ninth joint. The metastoma is elongate ovate, widest in the middle, with ends truncated. The anterior or narrower end is notched and minutely dentate. The genital appendages of this species, so far as they are pre- served in the material of the collection, are, with the exception of the part carried by the second sternite in the female, essentially like those of E. fischeri Eichw., as described by Holm (13). That of the female is the more complex and is carried partly by 1102 NEW YORK STATE MUSEUM the operculum and partly by the second sternite. The part car- ried by the operculum follows two subtriangular areas formed by a pair of sutures extending posteriorly from either side of the median lobe to meet the cleft, and extends considerably beyond — the posterior edge of the plate. It consists of a short sagittate base and a slender portion divided transversely into two im- bricating sections, each terminating in a short bifid expansion [pl. 24, fig. 5]. In E. fischeri there is a third part consisting of two, short, flat, diverging crura. As this appears to be a general feature in Eurypterus, it is probable that it exists in this species also. The part of the appendage carried by the second sternite is covered by that of the operculum. It lies in the median -cleft which extends through the posterior two thirds of the sternite, the anterior third of the two halves of this plate being fused [pl. 25, fig. 5]. It is slender, being about one fourth as wide as long and does not quite reach the posterior edge of the sternite. The anterior end is slightly constricted where it fuses with the sternite, and the distal is taper- ing. The male appendage is confined to the operculum. In the material of the collection is a single specimen showing [pl. 25, fig. 2] the exterior, the others showing the internal form only. It was evidently small, about one fifth the length of the operculum by which it is surrounded. | The body is covered with comparatively coarse, imbricating, erescentic scales, most distinct on the sternites and swimming arms. When the integument of the metastoma and paired ap- pendages are scaled away, there remains a punctate surface. The specimens found show that the size of these animals aver- ages from 20 cm to 30 cm. A fragment of the third joint of a swimming arm was found, however, which appears to have been part of an individual over 60 cm in length. Genus preryeotus Agassiz. 1839 Pterygotus monroensis sp. nov. Plate 24, fig. 7, 9 This species is founded on a single specimen, a cephalo- thoracic shield. The outline of this shield is semielliptic with Gee ee REPORT OF THE STATE PALEONTOLOGIST 1902 1103 the posterior edge noticeably incurved. The surface is moder- ately convex, and along the sides and front is a. threadlike border. The length of the shield, without the genal angles, is 30 mm, with them 37 mm; the breadth at the base 88 mm. The compound eyes are prominent and project beyond the outline of the shield. They are subelliptic, with a distinct angulation on the inner side of each, produced by an indentation of the inner anterior part. They are 14.5 mm long and 6 mm wide. The facets can be made out with a good magnifying glass. The eyes are located a distance equal to their own length from the front of the shield and 27 mm from each other. A line connecting their bases cuts the axial line a little back of the center of the shield. The ocelli are on a small tumescence just back of this. The ornamentation is almost obliterated, but can be made out at one point, where it consists of minute, short, flat, lobelike scales. Out of the eight species of Pterygotus that have been de- scribed from American strata, and all from the Bertie water- lime, the cephalothorax of but one has been identified, that of P. macrophthalmus Hall (10). Pohlman (14) described and figured one, but did not refer it to any species. It seems probable that it is of an older individual of P. macroph- thalmus. The cephalothorax of this new species differs from that of P. macrophthalmus in that its length is nearly equal to its breadth; the compound eyes are over one third the length of the shield, elongated, angulated on the inner side, situated farther back, and separated by nearly twice their length. In Eemacrophthalmus (15) the length of the shield is three fourths the breadth; the eyes are about one third the length of the shield, anterior, globular and separated by a distance about equal to their length. In form the eyes of this species suggest those of the erettop- terid species (subgenus Erettopterus Huxley), P. bilobus Salt. and P. banksii Salt. and also those of H. socialis. 1104 : - NEW YORK STATE MUSEUM Fragments of Pterygotus Plate 24, fig. 6, 8 In addition to the cephalothorax described above, other parts were found, mainly mere fragments, having the coarse, scaly orna- mentation of Pterygotus, but even the more perfect can not be referred to definite’ species, because of their isolated condi- tion. Among these is an ovate metastoma [pl. 24, fig. 8] 27 mm long and 16 mm wide, broadest just anterior to the middle, with the anterior corners slightly truncated, the lobes small and the terminal notch very narrow and shallow. It is marked by coarse, rounded, lobelike scales and is very much more robust than would be expected in Pterygotus mon- roensis. Judging by the ornamentation, it should be asso- ciated with the coarse scaled fragments most frequently found. The broken, free ramus of a chela of a Pterygotus is repre. - sented on plate 24, figure 6. The shaft is nearly parallel sided, 8 mm broad and 12.5 mm long and curves at the end into a stout, striated, nearly ‘perpendicular mucro 3.5 mm long. Back of this mucro is a series of 10 erect, subtriangular, striated - denticles, very slightly separated at their bases. They are of three sizes, the largest or primaries being about one half the | length of the mucro, the secondaries one half that of the pri- tmaries and the tertiaries about one half that of the secondaries. ‘The first primary is separated from the mucro by a secondary and from the second primary by two secondaries and two ter- tiaries alternating; following the second primary are two sec- - ondaries separated by a tertiary. He The free ramus of Pt. buffaloensis Pohiman (14) differs from this in having the shaft convex on the inner side; the teeth perpendicular, numerous, acute, varied in length, one or two longer ones about midway in the series; and the mucro set at an acute angle. a In P. cobbi Hall (10), the only other species of the Water- lime in which this ramus is known, it is many times larger than this fragment; shaft tapering; mucro less erect and blunt tipped; teeth six, comparatively short, strong and unequal. Another fragment [pl. 24, fig. 1] represents the basal part of the long, tapering, proximal joint of a chela of a Pterygotus. REPORT OF THE STATE PALEONTOLOGIST 1902 1105 These fragments show the genus Pterygotus to be fairly weli represented in the black shale by species, though not by num- bers. Genus ( ye Plate 26; fig. 1, An ae ceric differing very oranges from anything de- scribed from the Bertie waterlime, is represented in the collec- tion by a group of four incomplete arms and a body segment, and by another of two incomplete arms. In the first group [pl. 26, fig. 2] the longest of the arms has the coxal and succeeding five joints preserved. These are long, measuring altogether 110 mm in length. The three distal bear a series of long, curved spines. The form of the coxal joint is subtrapezoidal, the anterior side being considerably the longer. The breadth and the mean length are each about 18 mm. The dentate border is slightly produced and in length is equal to about one half the breadth of the joint. The denta- tion begins at the front end with an isolated, blunt tooth point- ing forward, followed by sharp, curved teeth of small size. which grade posteriorly into fine, hairlike bristles. The anterior side of each joint from the second to the sixth inclusive, is arcuate. The posterior sides of the second and third joints are straight, of the fourth, fifth and sixth, concave. The distal end of each is at right angles to the long axis. The second joint is nar- rower (14.5 mm) than long (23 mm); the third just twice as long (28 mm) as wide (14 mm); the fourth a little longer than the preceding (80 mm) and less than half as wide (7 mm). Along the concave, posterior side of the fourth are articulated five, long, curved, striated spines, nearly perpendicular to the joint. At the distal end of the series there is an indication of another. The most complete of these spines is 16 mm in length. The | fifth joint is 16 mm long and 6 mm wide. Near the anterior end of the posterior edge it carries the stump of a large spine fol- lowed by the sockets of four more. The sixth joint bears the basal portion of three spines, but is so crushed and fore- shortened that neither the original number of spines nor the length of the joint can be determined. Judging by the taper of _ this arm, there may have been two more joints. a 1106 NEW YORK STATE MUSEUM The remnant of another appendage appears to be part of the proximal four joints, and measures 32 mm in length. From its robustness, it seems to have belonged just in front of the last mentioned. The peculiarities of these joints are their shortness and their thickening ‘at the articulations. The joint, which on the tablet lies nearest to the large arm, is a little inflated and, though very imperrect, has the appearance of being the coxal joint. The two other appendases: of this group are robust and short. One is tolerably complete, apparently lacking only the dentate border of the coxal joint. It is 38 mm long and consists of seven joints. The coxal is large and globose. Each joint from the second to the fifth carries on the posterior edge a pair of short, stout, distally directed, lanceolate spines, averaging 2.5 mm long and nearly half as wide. Joint two is broad and very stout. Joints three, four and five are subquad- rate and successively smaller. Joint six is nearly one and one half times as long as broad and at the end bears two dis- tally directed spines, one anterior, the other posterior. The seventh is long and clawlike, slightly inflated at the base. The other appendage is so crushed and folded that little can be determined by it. However, from the larger size of the coxal joint, it is probable that its position on the body was behind the more complete. The spines preserved on it, like those of the smaller appendage, are short and lanceolate. The body plate in this group is very narrow (76 mm) as com- pared to its length (283 mm). Its division into right and left halves by a suture, the arching of each half and the produced anterolateral angles indicate it to have been a paired sternite. In the second group one of the imperfect arms consists of the four distal joints, the other of two imperfect proximal joints. The joints of the former are short and expanded at the articula-: tions. The first and second are each provided on the posterior side with a pair of distally directed spines. These are long, curved and sharp like those of the large arm of the other group. The second has also, on the opposite side of the distal angle, a single, large one extending parallel with the axis of the arm. The penultimate is long and shows no sign of having been REPORT OF THE STATE PALEONTOLOGIST 1902 1107 spiniferous. The terminal is about equal in length to the spines and, like the terminal appendage in the other group, is clawlike. This arm, judging from the shortness of the joints and the broad- ening at the articulations, probably corresponds to the second described from the other group. The joints of the other arm appear to correspond to part of joints two and three of the first of that group. Associated with this last, and lying partially beneath its larger end, is a fragment of test which is ornamented by sharp, triangular scales differing from anything found on the other eurypterids herein described. However, it is not certain that this had any connection with this arm. Aside from this possi- bility, neither the appendages nor the sternite show any signs of ornamentation. The most noticeable features revealed by these specimens are: the robustness and the great difference in size of the several pairs of endognathites; on the anterior three of these, the arrangement in pairs of the posterior spines, which, on the first two, are noticeable for their shortness and lanceolate form, and on the third for their length and curvature; the high degree of specialization of the fourth pair of endognathites, shown by the great length of the joints and the number and lerge size of the«spines; the narrowness and proportionately great Jength of the compound sternite; and the probability of there being several compound sternites. It is evident that the animal had a long, slender body with long, very strong limbs. From a comparison of these parts with those of the various genera of eurypterids, it appears that they do not agree very closely with any. To show this, it is necessary only to point out certain of the more evident differences. In Kurypterus proper the fourth endognathite, to which I consider the longer of these arms to correspond, consists of nine joints, probably a greater number than is possessed by the other; besides, it bears no spines except the two formed by the prolongation of the eighth or penultimate joint. On the three anterior pairs of endognathites the spines are more uniform in shape and 1108 NEW YORK STATE MUSEUM size. The body is proportionately broader and shorter than that indicated by the sternite described above. In eurypterids of the typeof Husarcus scorpionis Grote and Pitt (15), Carcinosoma newlini Claypole (16), Echinogathus clevelandi Walcott (4), Eurypterus punctatus Salter. E. scorpiodes Woodward (8), E. scoticus Laurie (17), etc., so far as material shows, the preabdomen is obese, the second pair of endognathites is the longest, and all four pairs with their spines are curved forward. In Sty- lonurus and the related genus, Drepanopterus (17), the fourth endognathites are without any elaborate development of spines, and in the former are greatly elongated. In Slimonia the first pair of endognathites is tactile, the succeeding three pairs are’ short, vary little in size and are all provided with small spines at the distal ends of the joints. In the Pterygotus the four pairs of endognathites are filiform, of nearly equal size and probably in all cases, spineless. It seems quite probable that, wath more perfect material, this form will be found to represent a new genus. References Whiteaves. Palaeozoic Fossils of Canada, v.3, pt 1. 1884 Hall & Clarke. Palaeontology of New York, v.7. 1888 Barrande. Systeme Silurien, v. 1, suppl. 1872 Walcott. American Journal of Science, v.23. 1882 Walcott. U.S. Geol. Sur. Bul. v.10. 1899 Beecher. American Journal of Science, v.12. 1901 Clarke. N. Y. State Paleontologist Report. 1901 Woodward. Monograph of the British Fossil Crustacea of the Order Me- rostomata (Paleontographical Society. 1866-77) | 9 Laurie. Royal Soc. of Edinburgh, Trans. v.37, pt 2. 1893] 10 Hall. Palaeontology of New York, v.83. 1859 11 Huxley & Salter. Mem. of Geol. Sur. of the United Kingdom. Monog, 1- 1859 . 12 Schmidt. Mem. de l’Acad. Imp. des Sci. de St Petersbourg, v.31. 1883 13 Holm. Mem. de1’Acad. Imp. des Sci. de St Petersbourg, 8e série. 1896 14 Pohlman. Buffalo Soc. of Nat. Sci. Bul. v.4. 1875 =, 15 Grote & Pitt. Buffalo Soc. of Nat. Sci. Bul. v.83. 1875 16 Claypole. American Geologist, Oct. 1890 17 Laurie. Royal Soc. of Edinburgh. Trans. v.39, pt 3. 1899 COON Oo RW Ne it Ledge of Cobleskill limestone at Schoharie N. Y. Hammer mark division from the Salina shales. PRELIMINARY OBSERVATIONS ON THE COBLESKILL (“CORALLINE”) LIMESTONE OF NEW YORK BY C. A. HARTNAGEL More than 50 years ago Professor Hall! described a fauna obtained from a thin mass of limestone outcropping near the base of the Helderberg at Schoharie N. Y., which, on account of its great abundance in corals, had become known as the Coralline limestone. This is the lowest of the many limestone formations in the vicinity of Schoharie. In its western extension it was traced by its characteristic fossils as far as Herkimer county. From the paleontologic and stratigraphic evidence furnished by the study of this limestone and also from a similarity in litho- logic features, Hall concluded that the “ Coralline” represented the attenuated eastern extension of the entire Niagara group as it then was known in western New York. The evidence for corre- lation furnished by the 25 species of fossils specifically identified from the “ Coralline” was somewhat meager. With the excep- tion of the corals, Spirifer crispus Hall was the only species described as identical with the Niagara fauna, and even that has been shown to be a variety. Besides one or two Species of Stromatopora found in this reck and having but little value in correlation, the abundant Favosites was identified as F.niagarensis (?), while Halysites catenulatus? Linn., which at this time was not known above the Niagara, was considered the most important of the fossil forms in the correla- tion of the two rock masses. The many characteristic species of the Niagara however were absent, while the “ Coralline” was characterized by a peculiar gastropod and cephalopod fauna, a feature noticeably absent in the Niagara of western New York. These discrepancies between the two faunas were observed by * Palaeontology of New York. 1852. 2:321-38, pl. 72-78. .*Grabau. Geol. Soc. Am. Bul. 11:352. * This fossil was known above the Niagara only in the sense that Hall regarded the overlying waterlime as Salina. Vanuxem had recorded this species from the base of the waterlime group and had given the position of the waterlime above the Onondaga salt group. This coral was identified by Van- uxem asCatenipora labyrinthica. Geol N.Y.3d Dist. 4th An. Rep’t. 1840. p. 376. 1110 NEW YORK STATE MUSEUM Hall, and he attributed these differences to the unlike conditions under which sedimentation took place and to the unequal depth of the sea. Happily, however, the “ Coralline” was described as a distinct formation. The position, in the rock series, given to the “ Coralline” at Schoharie appears to have been based chiefly on its relations to Vid Aha Mime soe Tentacusite Jue STORE Water fires rore Serves the overlying and underlying beds which Hall regarded as the Salina and the Clinton re- Spectively. With these deter- Salt group minations it was impossible to conclude that the “ Coralline ” was other than the Niagara. county (Alter Mather teu): (=m ie From its similarity to the Salina in western New York, the rock above the “Coralline” could be readily con- fused. But why the underlying shales, clearly resting on the Lorraine beds, were called Clinton was not explained. Mather! had already published a section at Sharon Springs, Schoharie co., where the Salina shales resting on the Lorraine beds and below the waterlime were designated as the Salt group, and Vanuxem? Hudson Slate rocks had shown the impossibility of any formation between the Salina and the Lorraine at the same place. He says: “The Onondaga salt group [Salina] and the Frankfort slate [Lorraine] are So near to each other, both being undisturbed, as to preclude every other deposit.” Though Hall states that the “ Coralline ” could be traced continuously from Herkimer county to Schoharie, it is very evident from the above citations as well as from his own published -sections,® that it could not be traced below the Salina, to which position it had been assigned. In each of the three sec- tions herewith given between Sharon Springs and Litchfield, Geol. N. Y. 1st Dist. 1848. pl. 25, fig. 3. ? Geol. N. Y. 3d Dist. 1842. p. 79. 3 Palaeontology of New York. 1852. 2:15. The first section given as in the town of Canajoharie, Montgomery co., must refer either to the section on Cana- foharie creek, near Cherry Valley in Otsego county, or more probably’ to the section north of Cherry Valley near Salt Springville, as the highest beds in the town of Canajoharie are the Lorraine. Likewise the section above Wick’s . Store cited as in Montgomery, is in Herkimercounty. This place is now known by the name of Deck. REPORT OF THE STATE PALEONTOLOGIST 1902 1111 Herkimer co., the Salina shales are given a position directly on the Clinton formation (op. cit.) : . The following sections show the order of succession, and the nature of the materials of which the group is composed, at dif- _ ferent localities, from its more easterly exposures to the Niagara river : The most easterly section I have been able to observe is one in the town of Canajoharie, Montgomery co.; though the succession is there very obscure, and the whole thickness less than 50 feet. 1 Drab colored layers of Onondaga salt group 2 A red, coarse sandstone (forming a terrace) with pebbles, and containing much iron ore 3 A space occupied by shales 4 Grayish sandstone, conglomeritic below and darker colored and laminated above 5 Oneida conglomerate 6 Shales of Hudson river group At Vanhornsville in the town of Stark, Herkimer co., the fol- lowing section is exposed, though somewhat obscurely. 1 Onondaga salt group ! 2 Red, coarsely laminated, friable sandstone, contain- | Clinton | group ing much iron ore, but no distinct beds | 3 Green shale with fossils Clinton 4 Red, diagonally laminated sandstone -( group 5 Grayish sandstone and conglomerate, with thin layers of green shale 6 Oneida conglomerate 7 Shales and sandstones of the Hudson river group Section above Wick’s Store, in the town of Stark, Herkimer co. 1 Onondaga salt group 2 Quartzose sandstone and conglomerate, forming the terminating mass of the Clinton group | 8 Thin bedded sandstone with fucoids, alternating | Clinton : with green shale | group 4 Red sandstone, diagonally laminated ® White sandstone with pebbles and green shale 6 Oneida conglomerate 7 Shales of Hudson river group 1112 NEW YORK STATE MUSEUM In Herkimer county the “Coralline” is found in close prox- imity to the Eurypterus beds, which represent the upper part of the Salina. And it is singular that here, where the Salina has a considerable thickness, the relations of these beds should not have been at least suggested. Vanuxem,! referring to the division line between the Salina and the Waterlime group in the eastern end of his district, repre- sented by Oneida, Herkimer and Otsego counties, says: ‘ There a brownish impure limestone is seen, often mottled, containing columnariae of a somewhat spherical form and about the size of an inch or more; also a few encrinital fragments, and a small orthocera, the species not named. This is the mass which sepa- rates the two groups, and forms the base of the Waterlime group.” Again? in speaking of the upper member of the Salt group, representing the Eurypterus-bearing bed of the Salina, he says: ‘“‘“Above the upper deposit there are irregular, light colored layers with globuliform columnaria and other fossils, which belong to the Waterlime group, or to an intermediate one which we do not attempt to establish.” It may seem at first sight that Vanuxem might have meant by the intermediate layer that portion which we term Rondout, holding a position between the ‘“ Coralline” below and the Manlius limestone above. It will be seen however that the Waterlime group as defined by Vanuxem consisted, in this part of the State, of three distinct divisions, included between the _ Eurypterus-bearing beds of the Salina below and the Coeymans limestone above. The divisions of the Waterlime group as given by Vanuxem are as follows’: “The first or lowest portion con- sists of irregular layers with globuliform columnaria; above which there is a drab colored series, followed by the upper blue or dark colored ones.” | The section as above given agrees essentially with the one at Schoharie, the lowest member corresponding with the “ Coral- line,” the drab colored series with the Rondout and the uppermost. blue or dark colored ones with the Manlius limestone. The only fossil mentioned’ by name as coming from the lower part of the M Geol. N.Y. 3d Dist. 1842.) 9p. 111: > Geol. N. Y. 3d Dist. 1842. p. 99. ’"Geol: N; Y. 3d Dist. 1842. ip: 212% REPORT OF THE STATE PALEONTOLOGIST 1902 1113 section was Globuliform columnaria, which undoubt- edly is the same as Favosites niagarensis ? Hall. . COL VMIN SF Fig. 2 Upper Silurie section at Howes Cave, Schoharie co. Other fossils are mentioned as occurring in the basal member, but they appear not to have been identified. Unfortunately, the studies of Vanuxem did not extend far east of Otsego county, and he did not cor- relate his sections in Otsego and Herkimer counties with those of Schoharie. It will thus be seen that, while Vanuxem recog- nized a section clearly above the Euryp- terus beds in Herkimer county, he did not realize that the lowest member of his Waterlime group was the continuation of the “ Coralline ” of Schoharie county. On the other hand, Hall recognized the “ Coral- line” in both Schoharie and Herkimer counties, but in the latter he, evidently, was not aware of its position with refer- ence to the Eurypterus beds. The sections as above given, together with the results of a recent examination of the so called Clinton and Niagara forma- tions extending from Schoharie into Her- kimer county, clearly show that there is no representative of the Niagara east of Herkimer county; while the study of a new collection of fossils from Schoharie county and a similar examination of collections from horizons clearly above the Salina in western New York, conclusively demon- strate that the “Coralline” of Schoharie county is of an age later than the Salina, and that the “Coralline” has in New York State a greater extent than the Niagara itself. The inappropriateness of the term Niagara as applied to the “ Coralline” has been recognized for some time by Dr Clarke. This, together with the incongruity of the word Coralline as a 1114 NEW YORK STATE MUSEUM stratigraphic unit, has led him to substitute for these unsatis- factory designations the name Cobleskill, as it is along this creek near Howes Cave that the outcrops of this limestone are most typical. , Section at Howes Cave The accompanying section will serve to indicate the strati- graphic relations of the Cobleskill at Howes Cave. Directly beneath the Cobleskill the Salina shales are exposed with a thick- ness of 34 feet. The contact with the Lorraine beds can not be observed at this place, but in the bed of a small stream 1 mile farther north the contact is seen to be deceptively conformable. From observations made at this place, the thickness of the Salina at Howes Cave can not be far from 40 feet. The characters of these shales are quite uniform. In color they vary from a light eray to green. They break readily and soon crumple. The most conspicuous feature is the presence of nodular iron pyrites in such quantities that at Schoharie they were once mined. These shales have been quarried and sold for plaster, but, unlike beds of the Salina of western New York, they contain only traces of gypsum. Their value-as a plaster seems to be due to the oxida- tion and decomposition of the iron pyrites, the sulfur of the pyrites combining with oxygen and water, forming sulfuric acid. The acid attacks the carbonate of lime present, forming lime sulfate, which, with the addition of two parts of water, gives gypsum. : Folding and slight displacements of these shales are often seen, specially near their lower portion. These, however, appear to be only local developments. There is no transition into the Cobles- kill. The line of demarcation is very strongly defined. The soft shales, weathering away beneath, sometimes leave the Cobles- kill as a projecting ledge. These same features are observed farther east at Schoharie, where the formation has a thickness of 27 feet, having thinned 13 feet in a distance of 5 miles. The most easterly extension of these shales that has been observed is near Gallupville, 5 miles east of Schoharie, showing that the extreme eastern extension of the great Salina beds of New York 1U.5S. N. Y. Sec. Rep’t. Regents Bul. 59. 1902. p. r42. Plate 2 Cobleskill limestone with underlying Salina shales at Howes Cave, Scho- harie co. REPORT OF THE STATE PALEONTOLOGIST 1902 1115 ean not be far from the town of Knox, Albany co., at which place it is quite likely that the Cobleskill slightly overiaps the Salina. Both of these formations are absent at Altamont a few miles far- _ ther east, and the Rondout is seen resting directly on the Lorraine beds. Rondout waterlimes Next above the Cobleskill is the Rondout waterlime, which at Howes Cave is 40 feet thick. The Rondout is transitional into the Manlius limestone above, as well as from the Cobleskill below. Hall?! has called attention to the fact that, while in western New York, where the Manlius is absent, the line of demarcation be- tween the Salina (Cobleskill or “ Bullhead” of Erie county) and the succeeding limestone (Onondaga) is very conspicuous, in eastern New York the Rondout, then regarded as the Salina, gradually gave way to conditions under which the Manlius lime- stone was formed. Regarding the “ Bullhead ” as Cobleskill, it will be seen that in New York, with the possible exception of Schoharie county, there appears to be no unconformity between the Salina and the overlying rock. The transition of the Rondout into the Manlius as observed in eastern New York is also to be noted at Cayuga lake, and these same conditions probably exist at least as far west as Seneca county, beyond which the Rondout and the Manlius have not been distinctly recognized. The transition from Cobleskill to Rondout is marked by a change from the limestone of the Cobleskill to the cement of the Rondout. The weathered surface of the upper portion of the Cobleskill varies slightly from the weathered Rondout, but fresh fracture clearly shows the distinctive character of the cement rock. The fauna of the lower Rondout, though much reduced in force, is distinctively a Cobleskill fauna. Uall found Haly- sites catenulatus in the Rondout of Herkimer county, and recently Prof. J. J. Stevenson? called attention to the fact that Favosites niagarensis Hall is found abundantly in the lower 3 feet of the Rondout (cement) at Howes Cave. The * Palaeontology of New York. 1852. 2:339. °N. Y. Acad. Sci. Ann. v. 13, no. 3, p. 365-66. 1116 NEW YORK STATE MUSEUM transition of the Rondout from the Cobleskill and the gradual passage into the Manlius were clearly recognized by Professor Stevenson, and, had he carried his observations a little farther, their true significance might have been realized. The gradual change from the Cobleskill, which he regarded as the Niagara, into the succeeding formations he explained by saying, “Itzis sufficiently evident that, while the great mass of Salina shales was in process of deposit in central New York and in much of the Appalachian region, the conditions within this portion of New York changed so gradually as to bring about only a slow disap- pearance of the fauna.” From similar observations, based on the section at Rondout N. Y., Messrs Ulrich and Schuchert! have correctly concluded that the so called “ Clinton ” of Schoharie county is really Salina. There is no doubt, however, that they did not properly construe the section at Rondout in assuming that the “ Coralline” as there developed is equivalent to the Cobleskill of the Schoharie section. It will be shown from the sections in Ulster county that, while the Cobleskill is present, the “ Coralline” of that region repre- - gents an age earlier than the Cobleskill. It may be here stated that, while Hall wrongly concluded as to the age and position of the Cobleskill in Schoharie county, he was more nearly right in his estimation of the age of the “ Coralline” of Ulster county, though his conclusion in regard to the latter evidently was based on the Schoharie section. Fossil localities of the Cobleskill in Schoharie county — The Cobleskill limestone is more or less fossiliferous through- out its extent in Schoharie county, and the following lists repre- sent the collections made from its various outcrops. The sections will be taken up in order, beginning with the most easterly and extending along the line of outcrop into the western part of the county. | By On the Stevens farm south of Shutter’s Corners and 3 mil east of Schoharie the Cobleskill is partly exposed for some dis- tance. This has proved to be the best collecting ground for ‘N. Y. State Paleontologist. An. Rep’t. 1901. p. 650 (foot note) REPORT OF THE STATE PALEONTOLOGIST 1902 1117 Cobleskill fossils that has yet been observed. The following species were obtained : 1 Acervularia (?) inaequalis Hall Favosites niagarensis? Hall Enterolasma caliculus Hall Stromatopora concentrica Hall S. constellata Hall Atrypa reticularis Linné Camarotoechia neglecta Hall Chonetes jerseyensis Weller Orthothetes interstriatus Hall Rhynchonella (?) lamellata Hall R. pisum Hall & Whitfield Spirifer crispus var. corallinensis Grabau S. eriensis Grabau Stropheodonta bipartita Hall S. textilis Hall | Whitfieldella nucleolata Hall Tlionia cf. canadensis Billings I. galtensis Whiteaves I. sinuata Hall Mytilarea sp. Pterinea securiformis Halli P. subplana Hall P. cf. subrecta Hall Tellinomya equilatera Hali — Bellerophon (large sp.) | Bucania sp. Murchisonia (?) terebralis Hall M. sp. Pleurotomaria sp. Poleumita cf. crenulata Clarke & Ruedemann Trochoceras gebhardi Hail T. turbinatum Hail Kionoceras darwini Billings Orthoceras trusitum Clarke & Ruedemunn O. (large) Cyrtoceras sp. undet. oma N HD oO KF W b WwWwWWwWWWNHDNDSNYNYNNYNYNNYNYHPHP KB HB ee Be AOR wWNHHPSCHMANAAAKRANHYHESwoemMmN®ATKRWNH OS 1118 NEW YORK STATE MUSEUM 37 Cornulites arcuatus Conrad 38 Beyrichia (2 species) 39 Calymmene camerata Conrad 40 C. niagarensis Hall 41 Dalmanites sp. undet. 42 Homalonotus sp. 43 Leperditia jonesi Hall 44 Lichas (Dicranogmus) ptyonurus Hall 45 Proetus sp. undet. At this place the three system cleavage has caused the upper part of the rock at several points to become broken, so that the appearance is not unlike piles of pebbles. These pebbles often yield choice fossils of the smaller species, while the larger species are sometimes found in sections, being cut by the formation of cleavage planes. This method-of weathering and in places the removal of the weathered material have left the harder portion, representing colonies of coral extending above the general sur- face of the rock. The appearance of these coral masses indicates that this was their original place of growth, and thus a locality favorable for the existence of other types of life illustrated by the fauna above given. That these coral beds were the habitat of many of these life forms is shown by the occurrence of Trochoceras gebhardi and large gastropods, resting on the summits of a. coral growth. These gastropods, in turn, are seen to be places of attachment for new coral polyps, thus finally embedding the shells in the coral mass. Trochoceras geb- hardi is also found as the nucleus of large concretions, the surrounding mass of which is made up largely of coral growth. Below, in the more compact portion of the rock, there is a layer in which Chonetes jerseyensis Weller occurs in abundance. Associated with this species were found two fine specimens of Calymmene niagarensis Hall, the pygid- ium-of Lichas (Dicranogmus) ptyonurus Hall, fragments of Homalonotus sp.; also a number of Proetus sp. and several specimens of the cosmopolitan brachiopod Atrypa reticularis Linn., which however is but rarely found in the Cobleskill. Fragments of a brachiopod which in general form REPORT OF THE STATE PALEONTOLOGIST 1902 1119 and surface markings strongly resembles Stropheodonta becki Hall have been found. They may however prove to be identical with S. textilis Hall. Halfway between the above station and Schoharie at the spring which gives rise to a small brook, the Cobleskill is exposed for nearly its entire thickness. The following species were collected. 1 Favosites niagarensis ? Hall 2 Stromatopora concentrica Hall 3 Camarotoechia neglecta Hall 4 Rhynchonella (?) lamellata Hall 5-Spirifer crispus var. corallinensis Grabau 6 Whitfieldella nucleolata Hall The outcrop on the hillside northeast of Schoharie has long been a favorite place for the collection of Cobleskill fossils. A number of years ago the Cobleskill was quarried here, principally for the construction of a stone wall at the foot of the hill. The following species have been identified from this quarry. pn Favosites niagarensis ? Hall Stromatopora concentrica Hall Hederella sp. Atrypa reticularis Linn. Camarotoechia neglecta Hall Orthothetes interstriatus Hali Rhynchonella (?) lamellata Hall Spirifer crispus var. corallinensis Grabau Whitfieldella nucleolata Hall Pterinea securiformis Hall Bellerophon auriculatus Hall Pleurotomaria ? subdepressa Hall Px SD: 14 Spirorbis sp. Trochoceras gebhardi Hall T. turbinatum Hall Cyrtoceras sp. wCma nam oF W b feb pe ek wreoro phot et DADA Orthoceras sp. undet. fel ies) Tentaculites sp. undet. iw) (=) Calymmene camerata Conrad Leperditia jonesi Hall bo jot 1120 NEW YORK STATE MUSEUM At Mix & O’Reilly’s quarry the contact between the Lorraine and Salina beds can be favorably seen. The following section was measured with the aid of Mr O’Reilly. From the top of Lorraine to base of the Rondout......... 33 Cobleskill.( partly . 404050 Favosites niagarensis?............ Halysites catenulatus............. Stromatopora concentrica......... Sconstellatas yeast a sues Lichenalia c7. concentrica.......... Atiy pa reticularis, 2s2.%j.selee. te: Camarotoechia neglecta........... Chonetes jerseyensis....... oer sake Leptaena rhomboidalis............ Orthothetes interstriatus.......... Rhynchonella ? lamellata.......... x xxx x XX x X xX x OP RST RER NIN xX EOS OOo < ESM Stropheodonta bipartita........... Sstenatilig gr. saccea tease iene anemia Whitfieldella nucleolata....:...... Mion ¢) scanadensisa” sti ene Te PmaGe Maisie 7 ners al eee inate eke Tssimuatas cs ae ee terse Seecee Pterinea securiformis............. P. sulbplamayy. ect ec ea stake Niae te Pi stibre tte). xteaie aavon se ate ote Tellinomya-equilatena..) .. 2 ias,.o° Bellerophon auriculatus........... Murchisonia ? terebralis........... Pleurotomaria ? subdepressa....... Poleumita ef. crenulata,.......... Trochoceras gebhardi............. SES Geir pti arta | a Go Nea eons Kionoceras darwinl.............. Oncoceras expansum.............. Orthoceras trusitum 2.2)... oe: Phragmoceras corallophilum....... Cormiullites arcuatuses 7's st. 2. Calymmene camerata.......... Seek Ch mila gareNSist ii 55. clone era ae eee Leperditia jonest, 5% ye ees TCSCOLATES 400.) Bion cars lous eee eae eee xX XK KX a xX exe ee Oe x xX x FIOOOOOD COE KOK K KX KKK OOOO KK KK EX x< ~ _ Includes also fossils from the lower zones of the Decker Ferry formation and the Wilbur limestone (‘‘ Coralline’”’ of Hall), which are below the Cobleskill. 7 REPORT OF THE STATE PALEONTOLOGIST 1902 1129 In the beginning of this paper I have called attention to the fact that the original fauna from the “ Coralline” limestone as described by Hall contained but little that was truly Niagaran in character. An examination, however, of the above list will show that the species which are known to occur outside of the Cobles- kill limestone are largely Niagaran species. In this case, how- ever, these Species are not indicative of the age of the Cobleskill, but must be looked on as the return of the Niagara and Guelph faunas after the long interval during which the Salina shales of central New York were deposited, and during which these faunas suffered such changes as time and environment would produce. A number of Cobleskill species continued their existence into the Rondout; and, so far as they have been observed, all the Species that have been found near the base of the Rondout, with — the exception of the Kurypterus, are forms also found in the Cobleskill, but none of the gastropods or cephalopods of the Cobleskill appear to pass upward into the Rondout. Cobleskill section at Union Springs, Cayuga lake The studies of Vanuxem extended as far west as Cayuga lake, the western limit of the third district. The last place where a line is sharply drawn between the Salina and the Waterlime rec- ognized as consisting of three groups, is at Waterville, in Oneida county. From that place to Cayuga lake only one locality is mentioned where the brownish limestone, so characteristic of the base of his Waterlime group in the eastern end of the district, follows the Salina. This locality is near Jamesville, in Onondaga county. A number of quarries are mentioned about Cayuga lake, and a final disappearance of the group under the lake. The stratigraphic position of these quarries, however, is not clearly indicated. In this connection it is interesting to note that Hall in speaking of the fourth or upper deposit of the Salina group, says :1 In Seneca county it does not appear in its usual characters; the _ highest rock of the group being a fine grained, dark colored, and grayish brown mass, which apparently represents the lower part 1Geol. N. Y. 4th Dist. 1843. p.129. 1130 NEW YORK STATE MUSEUM of this division. Between this and the succeeding limestone, there is an interval which is probably occupied by this mass, but. too deeply covered to be visible. It appears on the east side of Cayuga lake, coming down to the shore. As will be shown later, the grayish brown mass represents the Cobleskill, the covered interval the Rondout and the succeeding limestone the Manlius. . ? Attention was first prominently called to the section under con- sideration by the late Prof. S. G. Williams, in a Note on the Lower Helderberg Rocks of Cayuga Lake and in a paper on “The Western Extension of Rocks of Lower Helderberg Age in New York ”. published in‘the American Journal of Science? The sec- tion studied by Williams was in the vicinity of Union Springs and was included between the gypsum beds of the Salina and the Oriskany sandstone. From this section, having according to Williams a thickness of about 65 feet, he gives a list of 26 fossils, a number which were, according to the identifications, representa- tives of the Coeymans limestone and the New Scotland beds. It is. evident, however, that Williams did not examine the upper horizons of this section that lie directly beneath the Oriskany sandstone, or he could hardly have failed to find a nearly typical Manlius limestone fauna and thus perhaps have reached a differ- ent conclusion as to the nature of the fauna about Union Springs. Though Williams in his determinations of the fossil forms seems to have been supported by such authorities as Hall and Whit- field, there can be no longer any doubt that the fauna was not properly construed in assuming any definite biologic or strati- graphic relation to the Helderbergian series. The distinctively Siluric aspect of this fauna was first estab- lished by Dr Clarke,? who has also given considerable attention to the stratigraphy about Union Springs, which has resulted in accurately determining the position in the rock series of the out- crops on Frontenac island, from which the fauna of this section is mainly obtained. The accompanying map showing the geo- logic relations about Union Springs has been prepared by Dr 16th An. Rep’t. N. Y. State Geologist. 1897. p.10-12. *Ser.3. 1886. 31:189-45. *N.Y. State Mus. Mem. 3. 1900. p.99-101. ; 5 bo aie hs — Dy ota Bieta wet ee ea i iy a ss Oe et Ca a chal ry >) J =" ae wa ae ir re 7 7 ae ») ~ ah ; : z a A . Pod . P ; =- ; a a eal ; 2 ' 7%, “ r 4 \ fn ~~ 1 : Ld 7 - . ‘ j ‘ x yi & a ; y 4 ” 4 ) 5 ; ; \ ~~ B / ; : ; P 7 i } i Se a ea ia yr, JOHN M CLARKE STATE PALEONTOLOGIST STATE MUSEUM Antz f janes Anta /oofr.A.T S41 — —? SSS 00 Ft A:T Fae Section 25 Section 22.’ cg nae a ! Section 23 (See dolted line on upper secnen! Section! WE ——_ j Or anata BECRAFT MOUNTAIN Fess : : ’ _e* COLUMBIA COUNTY NEW YORK ee , a \ ‘ a 3 : tie {ADEUS W.GRABAT Section 24 LEGEND = - , HUDSON RIVER GRO! ens _ _ - - = — . ae | sa I . 2 = : b Sed bs UNIVERSITY OF THE STATE OF NEW YORK a : ANNUAL REPORT 1902 SECTIONS TO ILLUSTRATEH THE STRATIGRAPHY | | i fee a= Onondaga Schoharie Esopus Oriskany Port Pwen ecratt New Scoland Coeymans Maniius REPORT OF THE STATE PALEONTOLOGIST 1902 ist bite and Mr D. D. Luther, and it is with their permission that it is inserted in this paper. The collections from the waterlimes of eBay i New York by -Mr Luther and notes bearing on the region examined, have been made available for my study and have given valuable suggestions in working out the relations of the Cobleskill. The study of the fauna from Frontenac island (Union Springs) and its com- parison with the fauna of the Cobleskill of Schoharie county have had a very important bearing in showing that the “ Coral- line” or Cobleskill of Schoharie county is of post-Salina age. That a probable relationship existed between these two rock masses had already been suggested by Dr Clarke. In speaking of the species associated with the Eurypterus in the Salina beds of Cayuga and Herkimer counties, he says : The study of these has indicated the probability that we may not be altogether secure in the time-honored interpretation and correlation of some of our other strata having similar lithologic characters, such for example as the Coralline limestone of Scho- harie county and the waterlimes of the eastward sections. The fauna of a specially interesting outcrop of dark dolomite appear- ing on Frontenac island in Cayuga lake, where it is intercalated between the Waterlime strata, will, when fully studied, give important.aid in the interpretation of the proper relations of these beds to those which they immediately precede in time and to which they are otherwise allied, that is to the true Helderbergian strata. The probability of a relation existing between the beds of Frontenac island and the Cobleskill of Schoharie county, as thus expressed, may now be considered a certainty. As already indi- cated, the result given by Dr Clarke, relative to the unmistakable Siluric aspect of the section at Union Springs, is confirmed by a reexamination of the fauna, of which the stratigraphic relations, as shown by the accompanying map, can leave no doubt as to the position of these rocks with reference to the true Helderbergian strata. ™N. Y. State Paleontologist. An. Rep’t. 1902. p. 422. 1132 NEW YORK STATE MUSEUM Frontenac island The best location for the collection of Cobleskill fossils in the vicinity of Union Springs is on Frontenac island in Cayuga lake, about 14 mile from the village. This island, having an area of one half acre, is the remaining part of the south limb of an anti- cline, which has its axis extending in a direction a little north of east and passing through Hibiscus point, 34 of a mile north of the island. The upward flexure of the strata at Hibiscus point brings the gypsum beds above the lake level, but the dip on the north side of the anticline makes them again disappear below the lake at a point opposite the railroad junction. The surface of the island is nearly level and extends about 6 feet above the lake. 3 | The outcrops of the Cobleskill on the island consist of three strata of hard, dark magnesian limestone, having a dip to the south of about five hundred feet to the mile, thus bringing into view the three layers, which together have a Hips of 8 feet, 6 inches. The upper layer, which is soft and quite dark, has a thickness of 3 feet, 2 inches and breaks readily into small angular fragments. With the exception of corals it is the most fossilifer- ous layer. The middle layer which is 2 feet, 10 inches thick, con- tains Stromatopora in abundance and, except that the color is a little darker, it is precisely the same in appearance as the Stromatopora bed of the Manlius limestone, holding a position 60 feet higher. The two upper layers are quite uniform in color, which is well retained even after they have been exposed for a considerable length of time. The lower layer, with a thickness of 2 feet, 6 inches, weathers a lighter color than the upper layers, is less fossiliferous and approaches more closely the character of the underlying Eurypterus beds. | The Cobleskill limestone where exposed on the mainland is also fossiliferous, but no species were found that do not occur on the island. The following list therefore represents species identified from Frontenac island. 1 Chaetetes (Monotrypella) arbusculus Hall 2 Favosites niagarensis? Hall 3 Halysites catenulatus Linn. Oo Ot SD OO 10 11 12 13 14 15 16 17 18 19 20 21 92 23 24 25 26 27 bias 29 30 _— REPORT OF THE STATE PALEONTOLOGIST 1902 Stromatopora concentrica Hall Cyathophyllum hydraulicum Simpson Crinoid sp. Chonetes jerseyensis Weller ©. undulata Hall Rhynchonella pisum Hall € Whitfield Spirifer crispus var. corallinensis Grabau | S. vanuxemi Hall | Stropheodonta bipartita Hall S. textilis Hall S. varistriata Con. Whitfieldelia sulcata Van. Ilionia sinuata Hall Megambonia aviculoidea Hall Pterinea subplana? Hall Bucania sp. Cyclonema sp. Loxonema sp. Trochoceras gebhardi Hall Pleurotomaria ? subdepressa Hall Tentaculites gyracanthus Haton Gomphoceras septoris Hall Orthoceras trusitum Clarke & Ruedemann Orthoceras large sp. Beyrichia sp. Leperditia alta ? Hall L. cf. scalaris Jones 1134 NEW YORK STATE MUSEUM Distribution of the fauna from Frontenac island 2] 8 2 a pee % a8 q 3 ao | su = enlace r Smee |e /214|2 o 8 8 5 Sra os Chaetetes (Monotrypella) arbusculus...... x x Favosites niagarensis? 2s: 2 8 oe ose ee x x ? Halysites-catéenulatts:. 222 ah ee oe x x Stromatopora concentrica......:......... rR x x Cyathophyllum hydraulicum............. “aX Xx Chonetes jerseyensiss cic. sis sate esas tec x x C.andulatar i sss 4 tie eee ee Xx Rhynchonellanpisann: - sc er.ee ae eee x x Spirifer crispus var. corallinensis.......... x x 2 Sz VAMUReMT 4.46 pe oeee cs sce eis een nr or eee x x stropheodonta bipartita......2.2... 2.4: x x S. Gescbilig. bk ei Rae RNa ee eal epee eae x x De VETIStIAtG Foc.) Ue eae areorinians ade ne Xx x - Wehitheldella suleata-2 7 aes es x x x Thomiasimtlatiag so) 2) Gi i ec. aes teens ae x x x Megambonia aviculoidea................. XxX x Plerinea, subplanad.eacang uee oo eet x x x Trochoceras gebhardi... x x x x Pleurotomaria ? subdepressa eg hee Ah 2 x x Tentaculites gyracanthus................ x x Gomphoceras'septoris, = 22-2 (tee cee Der x e Orthoceras. frusitums: 25). 5 Gees oe ee x. x x Leperditia alta?....... aes Lhe EE EB os Xx x | hse osealaris. S20ee, 2, ihre eae een eee: x Xx | x The Cobleskill limestone appearing on Frontenac island also outcrops at the south end of Howland’s point, 14 mile northeast of the island. The dip here is greater than on the island and the outcrop less favorable for collecting. The surface layers how- ever contain large white Favosites, making a strong contrast with the dark color of the limestone. The surface as here exposed is in places polished and grooved by glacial action, thus indicating its resistant nature. A short distance from this outcrop on the northwest end of Howland’s point there is an outcrop of the Salina waterlime carrying Eurypterus and an undescribed spe- cies of Lingula. This outcrop of the Salina shows that the beds of Cobleskill on Frontenac island immediately overlie the Euryp- terus beds of the Salina. The Cobleskill limestone is also exposed in O’Connor’s old quarry 115 miles northeast of the island. The section in this REPORT OF THE STATE PALEONTOLOGIST 1902 135 quarry shows 6 feet of Salina waterlime, with 4 feet, 8 inches of Cobleskill. The Stromatopora layer forms the upper surface of the Cobleskill. é The location of this quarry is about 85 feet above the lake, which shows that the average dip of the Cobleskill is about 120 feet a mile. It should be noticed however that in this region the dip varies greatly. This is due largely to the fact that the flexures of the strata have been produced by two sources and at different times. One set of flexures evidently is produced by horizontal pressure resulting in a general tilting of the rocks, the other by vertical pressure: from below producing local disturb- ances, sometimes locally counteracting the effect of the general tilting of the strata and sometimes producing low conical eleva- tions, showing that the pressure was applied at a single point. The pressure producing these local disturbances appears to be due to the increase in bulk of the underlying beds, in the form- ation of gypsum from its anhydrite. These beds of gypsum ap- pear to be forming at the present time and they offer other inter- esting features, which can not be considered here. Excellent examples of these local disturbances can.be seen in the field just north of O’Connor’s quarry, where the Cobleskill is elevated into two cones, each having an elevation of 6 feet at the apex, where the rock is much broken and fissures are seen radiating from the center. A short distance northeast of O’Connor’s old quarry and at 15 to 20 feet higher there is another quarry in which 8 feet of Rondout waterlime is exposed. It will be seen from the position of these two quarries that the Cobleskill here holds the same posi- tion that it does in Schoharie county, namely, above the Salina and below the Rondout. The waterlime exposed in this quarry appears to be a good cement rock. It is dark in color, shows faint lines of deposition, and a tendency to split along these lines. A single segment of Eurypterus was found in the waterlime. exposed in this quarry. The Cobleskill limestone again appears in the old quarry on the land of Mr John Wooley, about 34 of a mile south of Cross Roads. The part of the limestone which is exposed, is hard. dark 1136 NEW YORK STATE MUSEUM in color and has a thickness of 4 feet. The Stromatopora bed forms the upper surface. Below the Cobleskill there is exposed 12 to 15 feet of Salina waterlime, which becomes laminated and shaly on exposure. In the Salina a short distance below the Cobleskill, Lingula sp. undet. occurs. . A cut on the Lehigh Valley Railroad, 14 of a mile east of Cross Roads station, passes through beds of gypsum at what is known as the Thompson quarry. Above the gypsum in the banks east of the pit, there are about 25 feet of Salina waterlime, overlain by the Cobleskill, which is here much folded and broken. The upper part of the Cobleskill is covered, but the overlying dark Rondout waterlime shows slightly in the top of the cut on the south side and in the field above. Near the middle of the Salina waterlime in this cut fossils are quite abundant. Several species of brachiopods and fragments of Eurypterus occur. The Lingula sp. undet. already mentioned as associated with the Eurypterus at Howland’s point, is found here extending to near the base of the waterlime. With the exception of a species of Leperditia, this Lingula appears to be the lowest fossil above the gypsum beds. The elevation of the Cobleskill in this cut is 510 feet A. T., which is 120 feet higher than Frontenac island. This outcrop in the cut however is on the other limb of the anticline, with a dip | strongly toward the northwest, showing that the actual dip of the rocks is much greater than the above figures would seem to indicate. | : Manlius limestone at Union Springs The best exposure of the Manlius limestone in the vicinity of Union Springs is in the J. S. Shaliboo quarry, 1 mile south of the village. The part of the Manlius that is exposed is directly below the Oriskany sandstone. The upper layer of the Manlius is 4 feet 5 inches thick and quite free from Stromatopora, but Leperditia alta Hall and a small species of Tentaculites are very abundant. The next layer below is a fine, dark blue limestone containing much Stromatopora. This is the layer which in appearance is similar to the middle layer of the Coble- skill on Frontenac island, to which reference already has been REPORT OF THE STATE PALEONTOLOGIST 1902 1137 made. The third layer contains less Stromatopora, while in the fourth layer it is absent. The lower layers weather nearly a uniform color. The following species have been identified from this quarry. 1 Chaetetes (Monotrypella) arbusculus Hall 2 Stromatopora sp. | 3 Orthothetes interstriatus Hall 4 Spirifer vanuxemi Hall 5 Stropheodonta varistriata Con. 6 Whitfieldella laevis var. ? 7 W. suleata Van. 8 Holopea antiqua Van. 9 Tentaculites sp. Cobleskill in Seneca and Ontario counties In going west from Union Springs the same stratigraphic relations continue over the eastern part of Seneca county, but in McQuan’s quarry, 11% miles southwest of Seneca Falls, there is a bed of waterlime lying directly below the Oriskany sand- stone. This stratum of waterlime, which is 11 feet thick, con- tains Eurypterus within 2 feet of the Oriskany and represents the Rondout. Below the Rondout there is a bed of dark blue limestone containing much Stromatopora in its upper part but much less near the base. This layer is 8 feet thick and much like the Cobleskill exposed on Frontenac island, to which form- ation it is referred. The Salina beds do not appear at this point, but at Seneca Falls the gypsum beds are overlain by Salina water- lime containing Eurypterus. The Stromatopora bed of the Cobleskill is covered at Seneca Falls, but it is evident from the position of these two sections that it is included between the Eurypterus bed of the Salina and the Rondout. Whether the Manlius limestone again appears west of Seneca Falls has not been satisfactorily established, though there are several. localities where beds somewhat similar to the Manlius limestone have been observed. Hall! mentions but a single local- ity west of Cayuga lake, where fossils characteristic of the Man- ~1Geol. N. Y..4th Dist. 1843. p.141-42. (1138 NEW YORK STATE MUSEUM lius limestone were found. This locality is in the town of Phelps, Ontario co. The thin layers in which the fossils occur are said to be directly above the Salina waterlime. The upper limit of the Salina as here given by Hall is not clear, since in Seneca county and at Union Springs the Cobleskill and the Rondout were included in the Salina. The fossils obtained by Hall from this locality were not well preserved, and the figures given are illustrations of typical Manlius limestone fossils from central New York and not of those that were obtained in Ontario county. Whatever the stratigraphic relations of these beds may be in _ the vicinity of Phelps, it is evident that, before the western limit of the county is reached, there is found a stratum similar to the “ Bullhead ”, lying directly below the Oriskany or below the Onon- daga, where the Oriskany is lacking, and that it occurs in this position at a number of points between Ontario county and Buffalo, at which it is better known than at any other locality. Cobleskill, or ‘‘ Bullhead” limestone, of Erie county The quarries of the Buffalo Cement Co. afford excellent expos- ures of the Cobleskill or “ Bullhead ” magnesian limestone. The Cobleskill lies directly above the kurypterus-bearing beds of the Salina and is transitional from them. According to a recent paper by Mr Schuchert! there is a hiatus between the Eurypterus- bearing beds of the Salina and the “ Bullhead” rock of Erie county. It is very evident however that the rocks between which the hiatus is said to occur are transitional, and that such a hiatus does not exist, nor would one have been considered by Mr Schu- chert had he correlated the “ Bullhead” with the Cobleskill instead of with the Manlius. The upper surface of the Cobleskill at Buffalo is very irregu- lar, evidently because of elevation and erosion during the interval extending from Cobleskill and lasting till late Oriskany time. Another feature of the Cobleskill at Buffalo is the deep vertical fissures, extending through its entire thickness and well down into the cement beds of the Salina. Attention has already been — ealled to similar fractures in the Cobleskill about Union Springs. 1U.S. Mus. Proc. 1902. 26:416. * s ai 5 ——— ee OS ee ee REPORT OF THE STATE PALEONTOLOGIST 1902 1139 Whether they were produced by similar causes, it is at present impossible to say. Grabau has expressed the opinion that those at Buffalo are probably due to an earthquake shock. Some of the fractures at Union Springs appear to be of recent origin, while those described from Buffalo must have been formed previ- ee eee — y <7 7? Ass fe te Zz = Onondaga ff MUMCAU72. _ | [|_—]_-=— Fig. 3 Dike through Cobleskill limestone, Buffalo cement quarry (after Clarke) ous to Oriskany deposition, since they are filled with sand typical of the Oriskany. The dikes in the Cobleskill at Buffalo have been described in detail by both Dr Clarke! and Dr Grabau.? The stratum of Salina waterlime that is burned for “ hydraulic cement” at Buffalo is slightly more than 5 feet thick. It con- tains a number of species of Eurypterus and a species of Lingula, apparently the same that is associated with the Eurypterus at Union Springs. There are also a number of other species of fossils described from the cement bed. The character of the Cobleskill limestone varies considerably in its extent in New York State. In Schoharie county, where corals are so abundant that often they make up a large portion N.Y. State Mus. Mem. 3. 1900. p.96-98. ?Geol. Soc. Am. Bul. 1900. 11:357-61 1140 NEW YORK STATE MUSEUM of the rock, it is a limestone. In the western sections, where the corals common to the eastern portion are very rare, it is a dolo- mite. The petroleum odor so characteristic of the Cobleskill in Erie county is not observed in the eastern sections. In Erie county the rock is filled with cavities, due to the dissolving out of the corals, but in Schoharie county the corals often appear to be the most resistant portion of the rock. In both sections the Coble skill is in some portions rich in iron pyrites. In the three sec- tions where the Cobleskill has been mainly studied it varies but little in thickness; at Buffalo it is 8 feet, 4 inches, at Union Springs 8 feet, 6 inches and in Schoharie county it averages 6 feet. In view of our present studies, the most interesting feature of the Cobleskill of Erie county is the fauna which it contains. Of this fauna a careful study has been made by Dr A. W. Grabau.} From this limestone he recognized 12 species, to which has been added a species of Favosites. The following species have been identified from the Cobleskill of Erie county. 1 Nematophyton crassum Penhailow Cyathophyllum hydraulicum Simpson Favosites sp. Orthothetes interstriatus Hall (= O. ee Whitfield) Spirifer eriensis Grabau Whitfieldella sulcata Van. W. nucleolata var. W. cf. laevis Whitfield Rhynchonella sp. 10 Loxonema ? 11 Pleurotomaria ? 12 Trochoceras gebhardi Hall 18 Leperditia scalaris Jones A rather minute analysis of this fauna convinced Dr Grabau that it was closely related to the fauna of the Cobleskill, or ‘“ Coralline ”, limestone of Schoharie county, a conclusion which is strengthened by a recent comparison of the two faunas. The following species are common to the Cobleskill of Erie and Scho- Oo ON D O18 FP W bd | Buffalo Geol. Soc. 1900. 11:351-55, 363-73. REPORT OF THE STATE PALEONTOLOGIST 1902 1141 harie counties. Orthothetes interstriatus Hall, Spirifer eriensis Grabau, Trochoceras gebhardi Hall, Leperditia scalaris Jones. Two species, Cya- thophyllum hydraulicum Simpson and Whitfield- ella suleata Van., occurring in the Cobleskill in Erie county, are also found in the Cobleskill at Union Springs. In the study of this fauna Dr Grabau obtained a good clue, which if followed would undoubtedly have enabled him to estab- lish the true position of the Cobleskill, or “ Coralline”, of Scho- harie county. Having followed however Hall’s correlation of the “ Coralline” as the eastern representative of the Niagara, he ‘concluded “that the Manlius (= Cobleskill) limestone fauna of the Niagara region is a late return of the Coralline limestone fauna, at the close of the long interval during which the Salina shales were deposited in the Siluric seas of this region.” Cobleskill of the Hudson river valley In the opening sentence of the original description of the ‘ Cor- alline” limestone Hall! briefiy refers to its occurrence in the Hudson river valley as follows: ‘In the neighborhood of Schoharie, and extending along the base of the Helderberg moun- tains and along the Hudson river, there is a thin mass of lime- stone, characterized by an immense number of corals, chiefly favosites, and which forms a band so distinct from any other limestone that it has been for many years known by this name.” Hall? makes another reference to the presence of this limestone in the Hudson river valley; he says “ The Coralline limestone exists in place at several localities on the east side of the Held- erberg, but I have had no opportunity of examining these places in detail. It is not improbable that many more species may be added to those already known.” _ The fauna of this limestone in the Hudson river section how- ever remained unstudied. Darton has given us much relative to the occurrence of this limestone in Greene and Ulster counties, Dale and Davis have each made mention of its presence in the quarries about Rondout where itis typically developed, but, so 1 Palaeontology of New York. 1852. 2:321. * Palaeontology of New York. 1852. 2:337. 1142 NEW YORK STATE MUSEUM far as I am aware, it has always been considered the equivalent of the Cobleskill, or “Coralline”, limestone of Schoharie county! Upper Siluric section at Rondout The following section at Rondout, from about the middle of “the Vlightberg ”, was measured with the aid of Mr P. E. Clark, mine superintendent of the Newark Lime & Cement Co. Included between the Coeymans limestone above and the Lower Siluric (= Normanskill?) shales we have: ° Feet Inches 1 Manlius. Three layers of thin laminated lime- stone, representing the “ Ribbon limestone” ono of some of the older writers....0....:..5..0%. 12 2 Manlius. Stromatopora la Vere) Or Petes se 7 3 Manlius. Banded limestone ............ mee 5 4 Manlius. Three layers of dark, thin bedded lime- stone. Spirifer vanuxemi and Ten- taculites gyracanthus are found in the basal members), S02 ees ee Ths eee 5 Rondout. The “paving block”......... Be cc tte a 5) 6 Rondout. The “prismatic” layer. Makes a good cement, but, together with the under- lying Leperditia bed, it is usually left to form the Wane TMB Ay Ql aes nace leyel cee a ee 4 8 7 Rondout. Limestone containing Leperditia.... 2 2 8 Rondout. Impure layer of cement known as the a 5 od 0 eee rie mek ACen stam nee Pema RB a I) | il 5 9 Rondout. Soft “gray cement”............... 3 1 10 Rondout. Hard “gray cement”.............. 5 7 11 Cobleskill limestOme 20... cack sseprd au ieee ee | te 12. Salinase ards “black cement vr ce ar aie rs oe rig aad 13° Salina “Soft black cement... vane 4 5 14 Salina. Wilbur jimestone (= Niagara or “Cor- — alline ” limestone of Hall and other authors).. a Mota Fes eG AE, Pa aoe chert see 78 9 1T am indebted to Mr Gilbert van Ingen for much information relative to the geology of the sections studied in Ulster county. REPORT OF THE STATE PALEONTOLOGIST 1902 1143 Feet Inches . The thicknesses by formations are as follows: _s 7 = py eerie Spiga a eas 287 6 MRR c cas web nia a veg S as baie wie 23 9 SUOMI eee pats cei wba 3 xin ape Ac Bes ein, oye sate bie: 3 i The Salina, including basal limestone............. 16 AcE I have already, in a previous paragraph, called attention to the fact that the position of the “ Coralline ” limestone at Scho- harie, as determined by Messrs Ulrich and Schuchert, is said to have been based on the section at Rondout N. Y. In making this determination, however, these distinguished workers in paleontology followed Hall’s correlation of this “ Coralline” bed as the equivalent. of the Cobleskill, or ‘“ Coralline,” of Schoharie county, an obvious error now that it is known that in Ulster county the Cobleskill belongs to a higher horizon than the so called “ Coralline”, and consequently the “Coralline” of the Hudson river valley really belongs to an earlier age. Starting from the type locality of the Cobleskill in Schoharie county, where its stratigraphic relations to the overlying form- ations are accurately known, the Manlius limestone can be traced continuously across the Helderberg and into Ulster county. In a like manner, the Rondout at the base of the Manlius can be traced, but it is not always so conspicuous, and specially in the Helderberg it has become very thin, still in Albany county at Altamont, Indian Ladder, New Salem and South Bethlehem it can be observed, and, since the Cobleskill and the Salina have thinned out, it rests directly on the Lorraine shales. Similar stratigraphic conditions exist in the vicinity of Catskill, Greene co., and southward from this place the Rondout becomes better developed, and good exposures are seen just north of West Camp in the cut of the West Shore Railroad. In Schoharie county the basal portion of the Rondout lying directly on the Cobleskill is burned for “hydraulic” cement, but in passing eastward over the Helderberg this cement bed thins out and is wanting for many miles. It comes in again before Ulster county is reached, and here, as in Schoharie county, it represents the basal portion of the Rondout as here defined. Throughout Ulster county this basal portion of the Rondout is 1144 NEW YORK STATE MUSEUM known as the “gray cement.” Directly beneath the Rondout, or “* gray cement,” the Cobleskill is found. The Cobleskill about the cement mines in Ulster county is known as the “ middle lime- stone ledge” and separates the Rondout, or “ gray cement,” from the underlying Salina waterlime locally known in Ulster county as the “black cement.” | In the quarries and mines at Rondout the Cobleskill is repre- sented by a thin layer of limestone 7 inches thick. This layer, separating the Rondout from the Salina, weathers to a gray color and is characterized by Rhynchonella ?lamellata Hall and a species of Leperditia. Southwestward from Rondout the Cobleskill thickens rapidly and at Whiteport it is 10 feet, at Binnewater 12 feet and at Rosendale 15 feet. The Cobleskill also thickens northward from Rondout, and at East Kingston it is found to have a thickness of 10 feet. The Cobleskill was also observed near Glasco, where some specimens of Proetus sp. undet. were collected. It also is seen in the vicinity of West Camp and northward toward Catskill. In the Rosendale-Whiteport cement region Darton! has referred to the Cobleskill, or ‘middle limestone ledge,” as follows: There are two cement beds in the Rosendale-Whiteport region, and at Rosendale the lower bed, or “dark cement,’ averages about 21 feet in thickness, and the upper bed, or “ light cement,” 11 feet, with 14-15 feet of waterlimestones intervening. In the cement region south of Whiteport there are two cement beds, the upper, or “ white cement,” having a thickness of 12 feet and the lower, or “ gray (= black or dark) cement,” 18 feet with 17-20 feet of waterlime beds between them. The Cobleskill limestone in the Rosendale-Whiteport region con- tains an immense number of corals and other species character- istic of this formation in Schoharie county; but Darton did not give any account of its “ coralline ” character in this section. As will appear later, the Cobleskill in the vicinity of Rondout seems to have been included by Darton with the Manlius or Tentacu- lite limestone. The Salina waterlime, or “ black cement,” is best developed at Rosendale, where it has a thickness of 22 feet, at Binnewater it 1N. Y. State Mus. 47th An. Rep’t. 1894. p. 528, 531. REPORT OF THE STATE PALEONTOLOGIST 1902 1145 is 15 feet and at Rondout 10 feet. It can also be seen at Hast Kingston, where it has a thickness of 10 feet. This bed can also be observed at Glasco and West Camp, at both of which it under- lies the Cobleskill. Below the Salina waterlime, or “dark cement,” is found the “ Coralline” of Hall and other authors. This limestone con- tains a fauna which is a mixture of Niagara and Cobleskill forms, and is indicative of the Salina age of this limestone. Over a portion of Ulster county this “ Coralline” limestone occupies a position between what is usually considered the Clinton forma- tion! and the Salina waterlime. In this sense this “ Coralline ” limestone has the stratigraphic position of the Niagara, but, as the waterlime, in age, appears to represent only the upper portion of the Salina and is transitional from the limestone below, it ap- pears best to consider this “ Coralline” of Salina age. In this paper this limestone is designated as the Wilbur limestone, since it was near Wilbur in Ulster county that Mather? in 1848 gave us the following interesting section, of which the Heer member is the Wilbur limestone. Feet 1 Fossiliferous limestone like the ‘“ middle limestone of eG e MM SET MMO UATUD aie, ci sc0's es ooo asians s S's sie aces pees 60 2. Fossiliferous limestone, different from the above and EPL EITC TS 0G) os 110 1 2 ee 50 3 Compact dark gray limestone (contains encrinal spines MEMES rt 220. SONGS OPS dete ioe Os 34 eeerme@cd srriped limMeStONe. . 2... 0. eee eee ee ees 20 PROC CR OLLY.). Wo. so wards oe des ste ee eevee cee ns 2 Secon) black “1IMESLONE. 2225... a. ocd a cc ee ole owe 1 fowement rock (gray), four strata............c600000 12 8 Black “coralline ” limestone (various Radiaria; Cyatho- phylla, Catenipora, etc.) [=Cobleskill limestone]... 8 9 Cement rock (gray to black) [= Salina waterlime].... 8 10 Limestone, dark colored, impure and _ fossiliferous ailing LimieSlONeles seus see cs Seek sk ca. an eee es 8 Thickness of limestones and cements........... 203 11 Hudson slates and grits, thickness unknown ; Though i in eastern New York the terms Clinton and Medina have been re- . tained, it is becoming increasingly evident that they are oe Salina age. ; Geol. N. Y. 1st Dist. 1843. p. 331. 1146 NEW YORK STATE MUSEUM From Rondout southwestward through Wilbur, the Wilbur limestone is exposed at a number of points and rests unconform- ably on the Lower Siluric (= Normanskill ?) shales. Still far- ther soutwestward along Rondout creek the Wilbur limestone is seen resting on the Clinton quartzite, but directly west, as at Whiteport and Binnewater, the Wilbur limestone is lacking, and the cement bed rests directly on the Clinton quartzite. At High Falls there is a fossiliferous bed between the cement and the Clinton quartzite, and it is referred to the Wilbur limestone. At localities where the Wilbur limestone or the Salina water- lime rests on the Clinton quartzite, there is no marked evidence of any unconformity, though the hiatus between them must have been considerable if this quartzite is to be considered as Clinton. Passing north from Rondout, the Wilbur limestone is exposed in an old tramway which leads to the Becraft quarries. Darton? at this point gives the thickness of the Wilbur limestone as 5 inches. My examination of this section does not in all respects — agree with Mr Darton’s. In describing the section above referred to, he says: The lower limestone members are exhibited lying on the Hud- son river slates in the railroad cut and some old cement openings near the turnpike. There is a 4 to 6 inch bed of impure, ferrugi- nous limestone containing Niagara corals. On this there lie 7 feet of dark gray limestones, impure near the base and for 2 feet toward the top. Two feet above their bottom is a fossiliferous layer containing Atrypa reticularis, a very unusual occurrence in this part of the formation. This limestone is over- laid by a 10 foot bed of cement rock, of which the upper 4 feet are of poor quality. Next above is a heavy mass of fine grained, dark colored, brecciated limestone, filled with a great variety of corals representing the Stromatopora layer of the Tentaculite (= Manlius) series. It has here the very remarkable thickness of 10 feet with only a few thin beds of typical Tentaculite mem- bers above. As the result of my examination of this section, I have con- cluded that the limestone beds containing Atrypa reticu- laris should be included with the Wilbur limestone, which 1N. Y. State Mus. 47th An. Rep’t. 1894. p.501. Camerata... 2220.08) doi ia bea ee ee ne | pA CINE MMT hes Ais Ser coy sr dy Be ates PAS Ides Ge ced dw Be ecm 5 be eX x x KXXKXXKXXKXX XK -KKKK KKK | Niagara x X xx An examination of the above faunal list shows at once that we have here an assemblage of species that strongly indicates that the Wilbur limestone is intermediate between the Niagara and the Cobleskill or, as already indicated, it is of Salina age. 1152 | NEW YORK STATE MUSEUM In Ulster county there is a space above the Wilbur limestone represented by the lower cement bed that, with the exception of Leperditia, is almost nonfossiliferous, but, when the Cobleskill is reached, we have again, in part, the Wilbur limestone fauna, but with a less proportion of Niagara species and with an increase of new forms that have not been observed in any formation below the Cobleskill. In the 42 feet of shales and limestones below the Cobleskill | of the Nearpass section in New Jersey there occurs a fauna which like that of the Wilbur limestone is Niagaran in charac- ter. In the latter section however the cement bed, so conspicuous below the Cobleskill, in Ulster county, is lacking, and the forma- tion is more or less fossiliferous throughout. Some of the layers in the New Jersey section are crowded with Leperditia strongly suggesting brackish water conditions, but to a much less extent than in Ulster county. The fauna of the Nearpass section has been studied with some detail by Weller,! and he was able to identify with more or less certainty 31 species that for the most part are well known Niagara species. Some of the identifications as thus made by Weller, presumably those of Niagara species, have been ques- tioned by Ulrich and Schuchert;? but, judging from the fact that we do have Niagara species below the Cobleskill in Ulster county and relying on the previous work of Weller, it would not be unsafe, I think, to assume that there is below the Cobleskill in the Nearpass section, as in Ulster county, a fauna with unmis- takable Niagara elements. One of the chief differences between the section in Ulster county and the Nearpass section is the development in the former of an extensive cement bed which is entirely lacking in the latter, but is represented by shales and limestones. In the Ulster county section the marine conditions during which the fauna of the Wilbur limestone flourished seem to have been followed by a period of nonmarine or brackish water conditions, during which the overlying cement bed was formed. This change in conditions of sedimentation caused an almost entire destruction of the fauna, 1N. J. State Geologist. An. Rep’t. 1899. p.7—20. *N. Y. State Paleontologist. An. Rep’t. 1901. p.650. REPORT OF THE STATE PALEONTOLOGIST 1902 1153 and in part accounts for the great abundance of fossils found at the top of the Wilbur limestone, where it grades into the cement rock above. In a like manner immense numbers of ostracods are found at the top of the cement at the juncture with the Cobleskill limestone. At the close of the Cobleskill there is an almost complete annihilation of the fauna. The nonmarine conditions of the Rondout were much more widespread in their influences than those during which the lower cement bed was formed, and throughout the extent of the Rondout in New York but few of the Cobleskill species pass upward into this formaticn. In some of the shaly layers at the top of the Cobleskill in Ulster county very many remains of trilobites and other fossils have been found, and somewhat similar conditions have been observed in Schoharie county. In the Nearpass section the conditions so affecting the faunas farther north are not so apparent, and the rock is of a more cal- careous nature throughout, and some of the species found in the lower part pass directly upward into the Cobleskill limestone. The age given to the formation below the Cobleskill in the Nearpass section as determined by Weller was the same as the Niagara. His determination, however, was made when the Cobleskill was supposed te represent the eastern extension of the Niagara. Still he showed that the Cobleskill can represent only the upper portion of the Niagara, and that it is transitional - from the underlying limestone and shales. As we now know that the Cobleskill is just aboye the Salina, the fossiliferous formation just below the 6 foot bed of Cobleskill in the Nearpass section will be considered of Salina age. The Bossardville limestone lying below these fossiliferous beds in the Nearpass section, is also considered of Salina age. The N earpass section as above construed, as well as the section in Ulster county, does not include any formation of Niagara age. The absence of the Niagara from these sections may in part be _ accounted for as follows. Beginning with Oneida sedimentation [fig. 4] we have each of the successive deposits overlapping the next older till the Niagara is reached. This series of overlaps is observed of the deposits in eastern New York laid down in the 115+ NEW YORK STATE MUSEUM < 5 Q S re ESOA OA LS aw v2} SG Fj ORISEA hE TO SCHOHARIE KINGSTON fe joke te é THES LDEABE A6/ LA /\/ COEYMANS ae a aS ee ns, Sa AL as a MAWNLILS UNION SPRINGS BUFFALO RONDOUT | MAWNL JUS — = COBLESKILL Se Wee SARIS | COBLESKILL UA WILB ? Poe AG BUEL PH CLINTON VIOWVE FR SIL GRIC ~SHALES: NIAGARA CLINTON EDINA ? M. ; MEDINA ONEIDA ONE/DA eon re eee eae eS eee Fig. 4 Diagram showing overlaps and succession of formations of the Mississippian sea and an early stage of the Cumberland basin REPORT OF THE STATE PALEONTOLOGIST 1902 1155 Cumberland basin! as well as in central New York laid down in the Mississippian sea.2 The overlapping of these deposits was caused by the gradual subsidence of a mountain barrier which separated the two basins, and which as subsidence took place caused the overlapping edges of the successive deposits in these two basins gradually to approach each other, the thinned edge of each resting on the Lower Siluric shales. At the close of the Clinton there was a reelevation of the barrier, and the Niagara deposits do not overlap the Clinton formation and rest on the Lower Siluric shales, but in central New York the eastern ex- tension of the Niagara is found resting on the Clinton. The effect of this uplift on the limits of the Niagara deposits in the Cumberland basin is not so apparent, but none seem to have been deposited in New York. From late Niagara time subsidence again took place, and the Salina deposits of the Mississippian sea in New York spread east over the Niagara and Clinton formations, and the thinned edge rests on the Lower Siluric shales. A similar condition of over- lap is found in the deposits of the Salina age in the Cumberland basin. In the region of the Helderberg the Salina deposits of the Mississippian sea are separated from those of the Cumberland basin by quite an interval, but in southeastern New York, where the barrier was lower, they must have been very close together, and the last deposits may have mingled and a few Eurypterus passed from the Salina sea into the Cumberland basin. With the clearing of the water brought about by the subsidence of the barrier, the Salina stage was brought to a close, and we have the Atlantic waters spreading over the late Salina sea. The spreading of the Atlantic waters over this area brought with them an Atlantic fauna. This invasion is known as the Helder- bergian, or it may be properly designated the Cobleskill invasion, since it was during Cobleskill time that we have the first invasion of an Atlantic fauna into the interior following the Salina age. This invasion of the Atlantic waters explains in part the deriva- tion of the fauna of the Cobleskill limestone as found in Sehoharie county. *N. Y. State Paleontologist. An. Rep’t. 1901. p.638. * Am. Ass’n. Adv. Sci. Proc. 1894. 42 :129-69. 1156 NEW YORK STATE MUSEUM Guelph element in the fauna of the Cobleskill limestone Mingled with the species of the Cobleskill derived from Atlantie waters, there are found in Schoharie county and westward a number of gastropods and cephalopods with some lamellibranchs, all of which in the eastern extension of the Cobleskill are con- spicuously lacking. An analysis of this element in the Cobleskill fauna shows that a number of the species are identical with Guelph species of New York and the West. Among these forms are found such Guelph species as Orthoceras trusitum Clarke & Ruedemann, Kionoceras darwini Billings and Tlionia galtensis Whiteaves and other species which appear in the foregoing lists. Species common to the Niagara and the Guelph and not observed in the Cobleskill of eastern New York occur in Schoharie county with the true Guelph species. There are also Niagara species in the Cobleskill found in the Niagara of the West, but which do not occur in the Niagara of New York. : The presence of Guelph species in the Cobleskill is accounted for as follows. At the close of the Niagara age there was an increase in the salinity of the water, which was the first step toward bringing about the conditions of the Salina sea. During this period following the Niagara, the Guelph fauna of New York flourished, but finally retreated as the sea became more saline. Again at the close of the Salina age, when in western and central New York nearly normal marine conditions had been established, the Guelph fauna returned and met the invading fauna of the Atlantic. The mingling of these two faunas shows that during Cobleskill time the waters of the Atlantic and the Mississippian sea were in communication. In the conclusion which I have reached relative to the mingling of these waters I differ from Ulrich & Schuchert,! who state that, though the barrier to the east was crossed, a younger fold “still prevented the Atlantic from joining the Mississippian sea throughout the time from Medina well into the Oriskany.” 1N. Y. State Paleontologist. An. Rep’t 1901. 1902. p.662. e REPORT OF THE STATE PALEONTOLOGIST 1902 1157 Rondout formation The mingling of the Atlantic waters with those of the Missis- sippian sea was of but short duration, and the Cobleskill was brought to a close by the formation of a barrier in western New York. This barrier as it grew caused a retrogression of the suc- ceeding deposits lasting into Devonic time and effectually sepa- rated the waters of the Atlantic from the Mississippian sea till late Oriskany time, when some of the Oriskany sand was de- posited in the crevices forming dikes and on the eroded surface of the Cobleskill. With the elevation of the Cobleskill in western New York, the true marine conditions under which the Cobleskill fauna flour- ished were also brought to a close, and in New York there was again formed a lagoon or bay in which the Rondout sediments were deposited. This bay was similar in some respects to the early Salina sea, but was diametrically opposite in that it formed an arm of the Atlantic instead of the Mississippian sea. The -conditions following the close of the Cobleskill were such that but few of the Cobleskill species pass up into the Rondout. That the Rondout was, unlike the Cobleskill, a nonmarine formation is shown by the return of the Eurypterus fauna, though much reduced in force. At Seneca Falls Eurypterus have been found in the Rondout but 2 feet below the Oriskany sandstone. They have also been observed in several localities about Union Springs and eastward. The writer has found Eurypterus remipes, in place near Cherry Valley at a horizon which may possibly prove to be the Rondout; and, till the exact horizon is determined, this find is chiefly interesting in that it is the most eastern locality in New York from which Eurypterus has been obtained. In eastern New York and the Helderberg the conditions favor- able for the existence of Eurypterus seem to have been lacking, at least none have been found indicating that these localities were in more direct communication with the sea. The fauna found at the base of the Rondout in the Helderberg sections is made up of species which continued their existence from the Cobleskill, and which do not pass upward into the Manlius lime- stone. In central New York there is a relation between the 1158 NEW YORK STATE MUSEUM faunas of the Rondout and the Manlius, and this relation is expressed chiefly by the passage of Kurypterus up into the — Manlius limestone. Hall! early called attention to the finding of “a specimen con- taining a part of the head of a Eurypterus and several impres- sions of a spirifer peculiar to the tentaculite limestone. The character of the rock is intermediate in color, texture and com- position, between the ordinary drab colored layers of the Onon- daga salt group, and those of the tentaculite limestone.” It is possible that the above specimen may have been obtained from the Rondout. Dr Clarke, however, has recently informed me that he has found Kurypterus in the blue layers of the Manlius limestone in Herkimer county. In Onondaga county, above the blue layers containing the typical Manlius limestone fauna there are two layers of “ Waterlime” from which the original “‘ water- lime of Manlius” takes its name. From the upper layer of this waterlime Luther? obtained a segment of a Eurypterus, showing that these interesting creatures continued their existence through all of late Siluric time, and that in this section at least there was an alternation in the character of the sediments and, as sug- gested by the fauna found in them. a considerable variation in the degree of the purity of the waters in which the sediments were deposited. | Culmination and decline of the Salina sea The occurrence of Guelph and Niagara species in the Cobleskill at the close of the Salina is very suggestive. The limits of the Salina deposits as now known are marked faunally by lower and upper Eurypterus beds, signifying that the period opened and closed under similar physical conditions. If, however, we start at the close of the Niagara period, we find the first indication of increasing salinity, and with this change came the Guelph? fauna. With the ever increasing salinity of the waters the Guelph fauna 1 Palaeontology of New York. 1852. 2: 339. ; 2N. Y. State Geologist. 15th An. Rep’t. 1898. p.268. This fauna, together with the environments under which it lived, has re- cently been studied by Clarke and Ruedemann, and is described in memoir 5 of the New York State Museum. REPORT OF THE STATE PALEONTOLOGIST 1902 1159 OO LDLCATL STING SALINITY SALINAS INCSIE ST SING SALINITY retreats, and next in the black Pittsford! shale at the base of the Salina there occur Eurypteri, and with them constantly asso- A WV ATT — SLB ag a a a FAUNA WATEFL MME C| Wit ELPYPTEFUS Lape Ia | (DY 7 g/l ty ai LELTD Ue i OD AV (Sy halt) OL bar Sill FS. eA OFELIA ALE VAISS POPP IP IESE OSS: SLE ee Md a FLYLLUN/T A MAGI T/7 Vata Fig. 5 Cycle of aa showing the culmination and decline of the Salina sea MA GST A ciated a species of Lingula. With the retreat of this fauna we find, as physical changes went on, deposits of gypseous shales 1'The Pittsford shale, which is exposed in the vicinity of Pittsford, Monroe co., is very dark and fragile, checking rapidly in drying. Intercalated in this shale are thin layers of gray dolomite carrying species similar to Leperditia scalaris Jones and Pterinea subplana Hall.=Leperditia scala- ris is a characteristic species of the Cobleskill in Erie co., while P. subplana appears to be represented in the Cobleskill of the Schoharie section. The eurypterid and pterygotid species of the Pittsford shale are described by Mr C. J. Sarle in the annual report of the ‘state paleontologist, of which this paper forms a part. 1160 NEW YORK STATE MUSEUM and later the salt beds. The deposition of these great beds of rock salt marks the turning point in this cycle, at which time the Salina sea contained very little if any water at all. With the increasing depth of the sea, beds of gypsum were again deposited, but never again were the conditions favorable for the deposition of extensive beds of rock salt. Following the gypsum beds, we have the Salina wateriime with its splendid Eurypterus fauna, and associated with the Eurypterus is a species of Lingula similar to the one at the base of the Salina. Above the Eurypterus beds we have the Cobleskill limestone, and here again we have repre- sentatives of the Niagara-Guelph fauna. Era or system | Period or group | Age or stage ( { Manlius limestone Rondout waterlime Cobleskill limestone Cayugan : (Neontaric) 1 Salina beds ‘ | Wilbur limestone, (Pittsford shale, L local facies) 1 Ontaric or Silurie { ( Guelph dolomite Niagaran Lockport limestone (Mesontaric) Rochester shale : Clinton beds | Oswegan Medina sandstone | (Paleontaric) Oneida conglomerate l Shawangunk grit Upper Siluric sections in Onondaga county The upper limit of the waterlime group of Vanuxem, in the eastern part of the third district was marked by the Coeymans limestone. At the type locality of the Manlius limestone in Onondaga county, where the Coeymans limestone together with the other members of the Helderbergian formation were sup- posed to be absent (not being recognized west of Madison county), the Waterlime group included all the strata up to the Oriskany sandstone. In the townships of Manlius and Dewitt, Onondaga county, the thickness of the strata from the gypsum beds of the Salina to the Oriskany sandstone is 190 feet. The lower portion fa ES hele EAA hee aaa 1 EE gn eLearn 1 Ontaric or Siluric of the New York series as modified from Science, Dec. 15, 1899. REPORT OF THE STATE PALEONTOLOGIST 1902 1161 of the section can be best studied in the vicinity of the Heard gypsum quarry 1 mile south of Lyndon in the town of Dewitt. The middle portion is best shown at Brown’s falls on the west branch of Limestone creek, 114 miles southwest of the village of Manlius, while the upper portions are made accessible by the natural outcrops and the extensive quarries in the hill just east of Manlius. Section at the Heard gypsum quarry Salina formation. North from the quarry there is exposed in the road and in the fields a dark porous limestone. In some of the thinnest layers Leperditia cf. scalaris is very abundant, while a small species of Whitfieldella is very common in the other portions of the rock. This limestone was formerly burnt for lime and its horizon is about 40 feet below the gypsum exposed in the quarry. The interval between this outcrop and the base of the gypsum quarry does not show any outcrop of the limestone. The gypsum including numerous intercalations of shale, is 65 feet thick and is overlain by 10 feet of olive-green shales which are quite soft, and often they lose their regular structure and become complicated, due largely to dissolving out of gypsum and to changes which have taken place in the under- lying mass. Above these soft shales there are 6 feet of Salina waterlime. The appearance of the rock is similar to the Salina waterlime of Herkimer county. Fragments of Eurypterus are frequently seen but the Lingula found at the same horizon farther west has not been observed. A small quantity of Salina waterlime taken out in the process of quarrying gypsum is now burned for cement, but it has never formed an important factor in the cement industry of Onondaga county. Cobleskill limestone. The Cobleskill limestone directly suc- ceeds the Salina waterlime. In this section the basal portion for 4 feet possesses the usual features of the Cobleskill of the eastern sections and is characterized by such fossils as S piri- fer crispus var. corallinensis, Whitfieldella nucleolata, Chonetes jerseyensis and Stro- pheodonta bipartita. The upper portion is transitional into the Rondout waterlime, from which it is not readily distinguishable. 1162 NEW YORK STATE MUSEUM Rondout waterlime. Only the basal portion of the Rondout is shown in this section. The rock here is brecciated and filled with cavities, some of which are quite large. Many of the smaller cavities are due to the dissolving out of the coral Cyathophyllum hydraulicum Simpson. In appear- ance this rock is similar to the “bullhead” rock of Erie county. The Rondout is burned to a small extent for cement, and then only when it is mixed with the cement rock of the upper horizons. The section as above given agrees essentially with one near Jamesville, published by Vanuxem.! Number 5 of his section is the Salina waterlime and according to his statement this was the only locality in the third district south of the Erie canal where cement was made from the rock of these lower horizons [p.110]. Number 6 includes what is now recognized as the Cobleskill limestone and the lower portion of the Rondout waterlime. The cyathophyllum mentioned by Vanuxem [p. 110] is unquestionably the one that is now identified as Cyatho- phyllum hydraulicum Simpson. The section given by Vanuxem is described under the third or gypseous deposit of the Onondaga salt group and is important in showing that in the type locality of the original waterlime group in Onondaga county not only Salina waterlime, but also the formations now known as the Cobleskill limestone and the Rondout waterlime, were included in the Onondaga salt group and not in the Water- lime group as has been generally supposed. Section at Brown's falls Cobleskill limestone. On the west branch of Limestone creek 114 miles southwest from Manlius village the Cobleskill lime- stone is exposed in the bed and banks of the creek 200 yards below the foot of the falls. The Cobleskill is here a compact limestone. The strata below the Cobleskill are only obscurely shown. Che Rondout waterlime. The basal portion of the Rondout is filled with cavities, and is similar to the lower portion as seen in- 1 Geol. N. Y. 3d Dist. 1842. p. 105. REPORT OF THE STATE PALEONTOLOGIST 1902 1163 the Heard quarry. The upper portion of the Rondout is com- posed of thin layers of impure limestones. The total thickness of the Rondout as determined at this section is 45 feet. Manlius formation. The lower portion of the Manlius is similar in appearance to the upper portion of the Rondout and gradually changes to the characteristic blue layers. The blue layers carry the typical Manlius fauna. In some of the layers fossils are exceedingly abundant, while in others they are rare. Some slabs contain an immense number of Spirifer vanuxemi and others contain equally large numbers of Leperditia alta. Tentaculites gyracanthus, so plentiful in the Helderberg section, is not found abundantly at Manlius. The Stromatopora bed of the Manlius occurs at the top of these blue layers just below the lower cement bed. In the eastern sections the Stromatopora bed is near the top of the Manlius not far below the Coeymans limestone. The thickness of the Manlius limestone up to the cement bed is 65 feet. The cement bed which follows the Stromatopora bed is 4 feet thick. No fossils have been observed in this layer. Above this cement bed is a layer of blue limestone 4 feet thick. Spirifer vanuxemi and Leperditia alta were obtained from this bed. The limestone is followed by another layer of cemeat 4 feet thick. Mr Luther records the finding of a segment of a Eurypterus from this upper cement bed in the quarry at Split Rock, south from Syracuse. The section above the cement beds can be observed in this vicinity but not so advantageously as in the hill east of Manlius. Section m the hill east of Manlus village The lower part of the Manlius limestone is not well exposed. It can be seen however at the cut of the Chenango branch of the West Shore Kailroad northwest from the station. In this cut there is a brecciated layer of limestone 1 foot thick. The rock in this cut and in the outcrops in the fields above is very fossili- ferous. The two layers of cement are well exposed in this hill where they are extensively quarried for cement. Above the upper cement bed there is an irregular layer of limestone 14 feet thick. In lithologic features it closely resembles the 1164 NEW YORK STATE MUSEUM Manlius. It is but sparingly fossiliferous and appears to be transitional into the Helderbergian to which formation it is provisionally referred. This blue limestone layer is followed by the Stromatopora bed 12 feet thick. The upper portion is very much broken by the formation of deep vertical fissures, similar to those seen in the Coeymans limestone. This Stroma- topora layer is referred to by Vanuxem [loc. cit. p. 110] where he says: “One of the layers, usually from four to five feet in thickness, is traversed by oblique cracks in at least three direc- tions, breaking the mass into irregular parts or fragments; this layer is very fine grained.” Besides Stromatopora found in this layer, corals of the genus Favosites are quite abundant. Spirifer cyclopterus is also frequently found. The Stromatopora bed is followed by 14 feet of massive blue limestone locally known as the “upper blue beds.” Fossils other than Leperditia are rare in these beds. Following these “upper blue beds” and directly below the Oriskany sandstone there is a massive gray limestone 6 feet thick in which some species of fossils are very abundant. This gray limestone ap- pears not to be present at all localities and where absent the Oriskany sandstone follows directly the “upper blue beds.” The following species were obtained within 8 feet of the Oris- kany sandstone. 1 Leptaena rhomboidalis Wilckens Orbiculoidea cf. discus Hall Spirifer cyclopterus Hall Stropheodonta becki Hall Trematospira formosa Hall Meristella c7. laevis Vanuxem Conocardium sp. undet. Pterinea communis Hall Oo ON ® oF WwW bD Tentaculites elongatus Hall Leperditia sp. undet. fot =) REPORT OF THE STATE PALEONTOLOGIST 1902 1165 General section at Manlius, Onondaga county 1 Oriskany. Fossiliferous sandstone, 6 inches to 2 feet ae thick ; 2 Helderbergian. Gray, compact fossiliferous limestone 6 3 Helderbergian. Blue limestone beds ................ 14 4 Helderbergian. Stromatopora beds, upper portion mue@n broken. 2... .: UAE PNR aed, AAR, RL at 12 5 Helderbergian? Blue limestone, fossils rare......... 14 6 Manlius. Upper waterlime bed. Eurypterus in this Pee ae rl OC?) Sota L OPA A OS 4 7 Manlius. Blue limestone with Spirifer vanux- Pemmand ele perdi ti ala lta ous. fees. oe: j 4 8 Manlius. Lower waterlime bed .................... 4 9 Manlius. Stromatopora bed at top. Blue layers be- low, containing typical Manlius fauna....... 2.6... 06. 65 10 Rondout. Upper portion, light weathering impure limestone; lower portion, a cement rock with MAM RR SRE Rtas Shi ice canbe, neh aeih hi 0d cA sMahiah MGs vb uekga tna evan 45 11 Cobleskill. Fossiliferous limestone gradually grading CLENG) ULES" LENO 615 (0) 1 ee ean ene ee rr 6 12 Salina. Waterlime with Eurypterus ................ 6 Pemaitd -eott, oreenish shales ... 2... a. sc eee oes 10 14 Salina. Gypsum beds, with intercalations of shale... 65 255 SUPPLEMENTARY NOTE While the foregoing pages have been passing through the press Mr Charles Schuchert! has published a paper “ On the Manlius Formation of New York.” The results obtained by Mr Schuchert and myself have been largely based on the same sections, though we differ considerably in our stratigraphic and faunal interpre- tations of them. As I have had recently an opportunity to examine the section about Litchfield, Herkimer co. it seems to me best to note in what respects we have differed in our sections and hence why we differ so widely in cur results, specially in regard to the grouping of the rocks under consideration, a differ- ence which to a large degree would have been avoided, were we more in accord in our stratigraphic and faunal determinations. American Geologist. March 1903. p.160-78. 1166 NEW YORK STATE MUSEUM Section near Port Jervis (Nearpass quarry section) For reasons which are more fully stated hereafter Mr Schu- chert proposed to include under the group term Manlius, the Manlius or Tentaculite limestone, the Rondout waterlime and the Cobleskill limestone as developed in the counties of Schoharie and Herkimer. In the section about Port Jervis it is very evi- dent that these limits have been greatly exceeded and that he has included with the Manlius, strata which contain a fauna that is unquestionably older than the fauna of the Cobleskill as devel- oped in its typical sections. Below the Cobleskill in the Near- pass section there are 42 feet of shales and limestones. “The diagnostic fossil of the lower half is Chonetes jerseyen- sis, otherwise the fauna is that of the Cobleskill member minus its corals” [p. 174]. It will thus be seen that not a single Niagaran species is recognized in this section since according to Mr Schuchert the Cobleskill contains no Niagaran species. This however is not in agreement with determinations made by Bar- rett, Weller and Whitfield, who have recognized Niagaran species therein. The Bossardville limestone at the base of the formation is correlated by Mr Schuchert with the Salina. Section at Rondout The Rondout formation as originally defined was intended to apply to the upper beds of the Salina characterized by an abund- ance of Eurypterus. Since it has been shown that at the type locality of the Rondout, the Wilbur limestone (= Coralline of Hall) is not the equivalent of the Cobleskill but belongs to an earlier age and stratigraphically lies below the cement bed of the Salina as well as below the Cobleskill, it follows that in its type locality the Rondout beds originally included the stratigraphic equivalent of the Eurypterus bearing waterlime of the Salina, the Cobleskill limestone and the Rondout waterlime as now restricted to that portion lying above the Cobleskill limestone. The re- stricted sense in which I have used the term Rondout may be the same as the intended use of this term by Mr Schuchert, but in the Rondout section he has failed to recognize the true Cobleskill, and hence his application of the term Rondout here is with its original limits and includes beds of Salina age, while in the other REPORT OF THE STATE PALEONTOLOGIST 1902 1167 sections cited by him it is restricted to the waterlime above the Cobleskill limestone. For the upper Eurypterus-bearing beds of the Salina Mr Schuchert uses the term Bertie formation which was introduced by Chapman in 1864. This formation strati- eraphically is equivalent to the basal portion of the original Rondout. Herkimer county section In the town of Litchfield the upper Eurypterus beds of the Salina are exposed on the farm of Prof. C. F. Wheelock. Near the outcrop of the Eurypterus beds, Wheelock’s creek has its origin. This creek flows north and joins Moyer creek near the point where the Oneida conglomerate outcrops. It is along Wheelock’s creek that the following section was observed. Oneida conglomerate. Basal member very coarse, resting on the Lorraine. After 5 feet of conglomerate there is an alterna- tion of sandstone and conglomerate which finally grades into the Medina. The pebbles are found quite abundantly for 45 feet. Medina sandstone. Above the conglomerate are about 70 feet of Medina sandstone. In his section Schuchert states that the Medina is absent. Likewise Vanuxem! and Hall? both state that the Medina is not found east of Oneida county. It should be observed, however, that Hall’s statement appears to have been based on the report of Vanuxem and the latter always considered - the Clinton as directly following the Oneida while the Medina was described as below the Oneida. A single quotation from Vanuxem’s report [p. 75] will serve to show that he regarded the Oneida as part of the Clinton. He says “ The conglomerate forms a part of the Clinton group, the next mass in order of super- position.” Clinton formation. The Clinton shales and sandstones are wéll exposed and have a thickness not far from 150 feet. Niagara formation. ‘The presence of the Niagara in this section is of special interest in showing that at one of the original locali- ties of the Cobleskill limestone we have both the Niagara and the Cobleskill present, being separated from each other by the entire Geol. N.Y. 3d Dist. 1842. p. 72. * Palaeontology of New York. 1852. 2:4. 1168 NEW YORK STATE MUSEUM thickness of the Salina, thus proving by the section along Wheel- ock’s creek the true stratigraphic position of the Cobleskill limestone. y In his section Mr Schuchert states that the Niagara is absent and that “Hall was able to find the Niagara formation as far east as Oneida county” [p. 162]. WVanuxem! records the pres- ence of the Niagara in Steeles creek, Herkimer county. This out- crop is about 3 miles southeast from the section under consider- ation, and its presence there is also recorded by Hall.2 The Ni- agara can be observed in place there on the right of the highway passing from Ilion to Cedarville. This exposure affords a favor- able opportunity to study the concretionary nature of the Niagara and its contact with the Salina shales. The Niagara has not been observed east of Steeles creek. There are some sections in western Herkimer and eastern Oneida where the Niagara is covered. Hall® states: “‘ Over a part of Oneida county _and the western-part of Herkimer, there is a space where no rep- resentative of the Niagara group has been traced continuously; not that the place where it should occur has been examined and found to be wanting, but because there are no good exposures of the strata which enable one to examine and determine satis- factorily the presence or absence of a thin bed like this one. In tracing the same line eastward however, into Herkimer county, there is a thin mass of limestone holding the same place, but more closely united perhaps with the drab limestone above, which is the thinned Onondaga-salt group.” The thin mass of limestone referred to is the Cobleskill. Tracing the Niagara from Oneida county eastward should have brought Hall to the expos- ure of the Niagara on Steeles creek, but at a point west of Steeles creek, he records the presence of the Coralline thus showing that the position of the Cobleskill as given by Hall was due to some extent to an error in correlation in Herkimer county. : In Wheelock’s creek the Niagara is thin, but the contact with the Clinton and the Salina can be favorably seen in the bed of the stream. The geodic concretions containing dolomite crystals, 1Geol.N. Y. 38d Dist. 1842. p. 91. * Palaeontology of New York. 1852. 2:107. ° Palaeontology of New York. 1852. 2:321. REPORT OF TH) STATE PALEONTOLOGIST 1902 1169 readily distinguish the Niagara from the adjacent rock masses. At this particular locality the base of the Niagara is a very dark shale, possibly the eastern extension of the Rochester shale. Salina beds. The red shales of the Salina are excellently ex- posed along the creek bed and highway which crosses the creek below Wheelock’s farm. A considerable portion of the upper Salina is not shown, but the Hurypterus waterlimes are exposed on the Wheelock farm. The total thickness of the Salina can not be much less than 50( feet. Cobleskill limestone. The best exposures of this limestone in the vicinity of the Wheelock farm is on the Augar and Morris farms, and in the highway 15 mile east of Wheelock’s. It is also exposed 2 miles east, not far from Steeles creek on the Kolb farm. There are other outcrops of the Cobleskill southeast from Wheelock’s near the Palmer cheese factory. Near the latter place the Eurypterus beds are shown in the highway and the Cobleskill outcrops just above, and for a mile frequent expos- ures are seen near the highway leading to Cedarville. The thickness of the Cobleskill in Herkimer county is given by Mr Schuchert as 30 feet, but I have not been able to find any outcrops where the thickness was so great. Hall states that in Herkimer county it is “only a few feet thick ” and observations made about the Kolb farm show a thickness of about 10 feet, though there are places where through the action of the “ creep- ing ” movement of the detached edge of the outcrop the thickness appears to be greater. The contact of the Cobleskill with the Rondout was advantageously observed at only one point. At the top of the Cobleskill Leperditia scalaris Jones anda large species of Beyrichia were found quite abundantly. Rondout and the Manlius formations. The combined thickness of the Rondout and the Manlius is about 100 feet. The Rondout is of a sandy hydraulic nature with but few fossils. In the thin sandy layers Eurypterus are cccasionally found. On one slab from the Rondout with Kurypterus there is found Rhyn- chonella? lamellata Halland Whitfieldella sp. The Manlius contains its usual fauna and in this section it is also characterized by many beautiful crinoids. The upper portion of 1170 NEW YORK STATE MUSEUM the Manlius becomes complicated with the Coeymans limestone, _ the faunas of these two formations either mingling or alternately recurring. Age of the shales below the Cobleskill at Schoharie The shales below the Cobleskill at Schoharie were desig- nated as Clinton by. Hall and now that we know that the Coble- skill is above the Salina the age of these unfossiliferous shales again comes into question. Mr Schuchert [p. 178] holds that “on the basis of the adjoining sections, the age of these olive green shales seems to be Lower Cobleskill.” What appears to be the chief argument, given for the determination of the age of the shales as Lower Cobleskill is as follows [p. 176]. “In Herkimer county the Clinton is not followed by the Niagaran, but at once by the Salina. Farther east the Clinton also fails, and at Schoharie, after 19 feet of the pyritiferous shales, there follow at once the Cobleskill, the Rondout, with the Coralline fauna, the Upper Manlius, and then the Helderbergian. Here the united thickness of the Cobleskill, Rondout and Upper Manlius is 91 feet, while about Litchfield the same zones are 110 feet thick. Therefore, the pyritiferous shale of Schoharie can not be the Clinton, but probably is the thinned eastern edge of the lower part of the Cobleskill of the Litchfield section and not of the true Waterlime or Bertie formation.” Even if we grant the thickness of the Cobleskill in Herkimer county as 30 feet, I am unable to see how the shales at Schoharie can be the thinned eastern edge of the lower part of the Cobleskill. If 19 feet represented the total thickness of the shales at Schoharie, this if added to the Manlius group of Schuchert would give about. the same thickness as in Herkimer county. But as a matter of fact the shales below the Cobleskill at Schoharie have a greater thickness than that given to the Cobleskill in Herkimer county. The shales therefore can not represent the thinned eastern ex- tension of the Cobleskill. Again in Schoharie county at Howes Cave the thickness of these shales is about 40 feet, which if added to the Manlius would give in Schoharie county a much greater thickness than the Manlius of Herkimer county .as defined by Schuchert, thus showing more conclusively that the REPORT OF THE STATE PALEONTOLOGIST 1902 a by | shales of the Schoharie section are not the thinned edge of the Cobleskill of Herkimer county. I am of the opinion that the pyritiferous shales of the Schoharie section can not be of an age later than the Eurypterus beds of the Salina. In western New York we have the Cobleskill following directly the Eurypterus beds. The transition from the one to the other has previously been noted. Specimens of Eurypterus from the Salina water- lime of Erie county have associated with them Orthothetes interstriatus and Leperditia scalaris, two fos- sils common to the Cobleskill from Schoharie county westward. At Union Springs somewhat similar conditions exist, while in Herkimer county the Eurypterus beds are also in close proxim- ity to the Cobleskill. These observations together with an examination of the section at Sharon Springs makes it difficult _to conceive how the shales of the Schoharie section can be other than the Salina. The formational term Manlius The term “ Waterlime group of Manlius ”’ was introduced by Vanuxem! and takes its name? from the two layers of water- lime lying above the horizon of the blue limestones containing the typical Manlius limestone fauna. That is we have in New York State three distinct waterlime horizons, (1) the Salina waterlime below the Cobleskill, (2) the Rondout waterlime above the Cobleskill and (8) the Manlius waterlimes above the horizon containing what is now recognized as the Manlius limestone fauna. These upper layers of waterlime are of a somewhat local development, a fact that was not clearly brought out by Vanuxem and thus has arisen much confusion relative to the position of the several cement horizons and they have generally been treated without much regard to their stratigraphic rela- tions. It should then be observed that included in the upper portion of the original Manlius is a waterlime and that the group was made to include all the waterlimes of the vicinity having a commercial value and not founded on any exact or even ap- proximate stratigraphic or paleontologic determinations. It “13d Annual Report. 1839. p. 272. Geol. N. Y. 3d Dist. p.110. N.Y. State Geologist. 15th An. Report. 1898. p. 267. 1172 NEW YORK STATE MUSEUM will thus be seen how the Manlius or Tentaculite limestone with its distinctive fauna came to be included with the waterlime group. In the final report of the third district Vanuxem! does not use the term Waterlime group of Manlius but simply Waterlime group. The fauna cited by Vanuxem is that of the Tentaculite limestone of Gebhard and Mather. In 1899 when it became de- sirable to substitute for Tentaculite limestone a locality name, Manlius was the term chosen, and as defined by Clarke & Schuchert? it is the equivalent of the “ Tentaculite limestone of Gebhard, Mather and later writers.” Since it has been shown that at the type locality of the Manlius the Cobleskill was included with the Salina it is in the latter sense that I have used the term Manlius throughout and always as a unit, though I have realized that the original waterlime group in the eastern portion of the district provisionally included the Cobleskill. Vanuxem? there referred what is now recognized as the Cobles- kill to the waterlime group or to an intermediate one which he did not attempt to define. The Manlius waterlime was never strictly defined and Hall* regarded it as a superior mass and above the strata containing the typical fauna. Consequently in the eastern portion of the fourth district the Onondaga salt group included all the strata up to the Manlius limestone. The Salina group as thus construed by Hall in this portion of the State may have had much to do with his calling the waterlime above the Cobleskill in Schoharie county Salina, since it occupies the same position stratigraphically with reference to the Manlius limestone. Among the chief reasons advanced by Mr Schuchert for in- cluding the Cobleskill with the Manlius formation is the state- ment that the fauna of the Cobleskill does not contain a single Niagaran species, while it does contain a few species in common with the Manlius. I agree fully with Mr Schuchert that the Cobleskill and the Manlius contain species in common and I have 1Geol. N. Y. 8d Dist. 1842. p. 110. * Science, Dec. 15, 1899. 5Geol. N. Y. 38d Dist. 1842. p. 99. 4 Geol. N. Y. 4th Dist. 1848. p. 128, 129, 141. REPORT OF THE STATE PALEONTOLOGIST 1902 ries shown more species in common to the two formations than has he, but I do not agree with him that the Cobleskill is without Niagaran elements. The evidence I have presented indicates that the Cobleskill fauna is tue last return of Guelph and Niagara species, and with the close of the Cobleskill the last Niagaran species disappears. The presence of these important Niagaran— elements justifies one in keeping the Cobleskill formation distinct from the Manlius limestone. The use of the term Manlius in the broad sense proposed by Mr Schuchert involves the duplication of terms, a feature which should be reluctantly accepted even if the stratigraphic and paleontologic interpretations could be considered correct. Additional note The fauna of the Cobleskill limestone of New Jersey, together with that of the underlying shales and limestones which are considered of Salina age has recently been described and illus- trated by Weller.2 The formations studied lie between the Rondout formation and the Bossardville limestone and are de- scribed under the name Decker Ferry formation, which Weller believes is the southern extension of what is now recognized as the Cobleskill limestone of Ulster county. This formation is best exposed in the Nearpass quarry near Port Jervis. The number of species identified from this formation is 48. Six of the species previously known were described from the “Coralline” of Schoharie county by Hall, one Chonetes jerseyensis is found in the Cobleskill in Schoharie, Herki- mer, Onondaga counties and at Cayuga lake. The species now recognized as Proetus pachydermatus Barrett has been obtained from the Cobleskill in Schoharie and Ulster counties. Hight of the species, Favosites pyriformis mai Halysites catenulatus Linn, Atrypa retic- ularis Linn, Leptaena rhomboidalis Wilck.,, Orthisflabellites Foerste,Reticularia bicostata Van., Pterinea emacerata Con. and Pterinea sub- plana Hall, are known from the Niagara of the interior but * Science, Dec. 15, 1899. p. 975. ' *Geol. Sur. N. J. Report on Paleontology. 1903. 3:62-75. 1174 NEW YORK STATE MUSEUM ~‘ of these three are not identified with certainty. Two species are identified as MHelderbergian forms—Pholidops ovata Hall and Rhynchospira formosa Hall. Among the species described as new Favosites corrugatus ap- pears to be the same as F. niagarensis? Hall (—F. hel- derbergiae var. praecedens Schuchert), a coral found abundantly in the Cobleskill. Another species Rhynchon- ella agglomerata is the same as Rhynchonella? litchfieldensgisg Schuchert. Both authors note a similarity of the latter species to the Niagaran form Camarotoechia neglecta Hall, to which species it was referred by the writer. Of the other forms described Cladopora recti- lineata Simpson, Monotrypa corrugata Weller, and Wilsonia globosa Weller are found in the Wilbur limestone. A study of the Leperditia of the Ulster county sec- tion will undoubtedly show that it has a number of species in common with the Decker Ferry formation. The evidence furnished by the study of the Decker Ferry fauna Shows that only the upper beds may be definitely correlated with the Cobleskill limestone. Though Weller states that [loc. cit. p.18] “the Decker Ferry formation, as well as the sub- jacent beds down to the Medina formation, were probably con- temporaneous with some portion or the whole of the Niagaran formations of the interior,” it can not longer be so considered _ since it has been shown that in the section along Wheelock’s creek in Herkimer county the original “coralline ” limestone is separated from the Niagara by the Salina, the latter having a thickness of more than 400 feet. It is evident that whatever elements we find in the fauna of the Decker Ferry formation, which are suggestive of Niagaran age, they must be looked on as a late return of Niagaran species. The fact that the Decker Ferry formation was, in part, deposited in a basin distinct from that in the interior accounts for variations in the faunas of the stratigraphically equivalent beds in central New York. Schuchert! includes all of the Decker Ferry formations under the term Manlius and Weller states that the Cobleskill at Ron- * Am. Geol. Mar. 1903, p. 174. REPORT OF THE STATE PALEONTOLOGIST 1902 1175 dout is believed to represent the extension of the Decker Ferry formation, in which case the lower cement bed at Rondout may be correlated with the Bossardville limestone. It is clear how- ever that the Bossardville limestone can not be correlated with the lower cement bed at Rondout since below the latter formation we have the Wilbur limestone with a fauna similar to the lower Decker Ferry fauna, which unites it with that formation and therefore the lower cement bed included between the Wilbur limestone and the Cobleskill limestone must be regarded as the stratigraphic equivalent of a portion of the Decker Ferry forma- tion. The presence of Leperditia and other fossils in the Bos- sardville limestone which lies just below the Decker “erry forma- tion is indicative of the Salina age of this formation. In Ulster county the Bossardville limestone can not be recognized, but holding a similar stratigraphic position there is a series of soft _ greenish shales and quartzites which are usually referred to the Clinton formation, but which, together with the underlying red shales, as has been already suggested, may more properly be referred to the Salina. DISTURBED FOSSILIFEROUS ROCKS IN THE VICINITY OF RONDOUT N. Y. BY GILBERT VAN. INGEN AND P. EDWIN CLARK With 13 plates ieee The present. paper describes briefly some of the more import- ant stratigraphic and tectonic features observed by the authors during several years work in the vicinity of the cement mines at Rondout N. Y. It is a statement of progress of investiga- tions now being carried on and is submitted with the object of bringing to the attention of geologists the highly er te fea- tures of that region. Several writers have published short papers on. the region, but these have evidently been based on far too hasty examina- tion, with the result that, while the more evident features have been Gescribed, numerous far more interesting though often less easily recognized phenomena have escaped attention, and the paleontology has been entirely neglected. The particular district described embraces the hill called the Vlightberg in the city of Rondout, on which are located the quarries and mines of the Newark Lime & Cement Co., and also that wooded range of hills, referred to in this paper as the North hill fronting the Hudson river and extending from the Vlightberg northward to the Terry triangulation station of the United States Geological Survey situated on the hill west of Terry’s brickyard, about 1 mile north of Kingston Point. This area, about 114 miles long by 44 mile wide, has been the scene of quarrying operations during the past 60 years, and the open- | ings, which in the Vlightberg are common along the eastern por- tion of the hill, afford unusual opportunities for observation of the interesting and complex tectonic phenomena in which the region abounds. Folds, faults and overthrusts can be seen in almost diagrammatic clearness. Up to the present time almost nothing has been done toward description of the fossil faunas of Ulster county, and as the Rondout region affords excellent opportunities for collecting fossils from the various members of the Siluric and Lower Devonic formations, a consideralle x ‘ae ag “a. > = - Plate 1 a tS ve S q I ss S. aS — isa 0 tL - \ \ is ~ SNe eave Mew = s) ~ C] > ir \ 4 > \ 7. YS Kea... } }} \G —< > Ako, Ip SS ia aS wi, aor 4 QS Bes Le <— DAO . RSE Sy S —= * = re 8 =e ; RS S; : a = St ZadN W REARS AI mS) wr, Ne: S) wag 7a 3 10" ‘e fe 4 y Li; a PX Na iy { (e Le << Z) oS SS r S a\">- Yj ‘ \ ao WES \ Contour interval 20 feet. Q Datum is mean seu level. oh ay Wee seer é 4 er Via . REPORT OF THE STATE PALEONTOLOGIST 1902 aia ave amount of material has been gathered by the senior author and the species have been identified to furnish the faunal lists accompanying this paper. One of the striking results of this paleontologic work is the discovery that a large number of those species heretofore considered to have been characteristic index fossils of the various members of the Helderbergian group are not confined to particular stages but range throughout two or more members of the series. The senior author, Mr van Ingen, first became acquainted with the region in 1888, and has visited it frequently since that date. The junior author, Mr Clark, has been superintendent of mining operations for the Newark Lime & Cement Co., for ‘several years, and in that capacity has had fine opportunities to study the folding and faulting of the formations beneath the surface. ‘In many cases the underground observations, supplementing the surface work, have enabled the authors to satisfactorily explain difficult points which could not have been solved by observations on the surface alone. | The structure is in places so complicated by excessive folding and faulting that it has been found necessary to prepare a large scale map. This map, still in manuscript, with a scale of 100 feet to 1 inch is based on stadia survey with the stations gener- ally less than 100 feet apart, and all outcrops are tied up to sta- tions. In this way the construction of parallel cross sections at frequent intervals will be facilitated, and reproduction of the tectonic features of the region by a series of models will be made possible. While both authors have been closely associated in the study of the structural features, Mr van Ingen alone is responsible for the paleontologic portion. The authors wish to acknowledge their indebtedness to Mr Calvin Tomkins, president of the New- ark Lime & Cement Co., for many favors extended them during the progress of their investigations. | | The visitor who approaches Rondout by boat on the Hudson river has his attention atiracted by a prominent hill which rises steeply back of the lower town to hights of 250 to 300 feet. This is the Vlightberg and the steep cliffs on the side fronting the river are largely due to the quarries opened along the beds of 1178 NEW YORK STATE MUSEUM waterlimestone which have during the past sixty years or more been mined here for use in cement manufacture. The Vlight- berg, with a length of about 14 mile and a width of 1% mile, lies with its longer axis in a northeasterly direction in the city of Rondout between Hasbrouck avenue on the southwest and Dela- ware avenue on the northeast, and constitutes a prominent ridge which separates the southeasterly portion of the city of Kingston into two parts, an eastern part known locally by the old name of Ponckhockie, built on the plain near the river, and a western part, Rondout, occupying the valley south and west of the Viight- berg. To the northward of the Vlightberg, the ridge is continued through the wooded “ North hill,” for about 2 miles to the vicinity of East Kingston where it becomes less prominent. At various points throughout its course its eastern face is very steep, as at “steep rocks,” and near Terry’s brickyard, and at a point east of Cloonan’s quarry, indicated on the map by ©, Delaware avenue passes across the ridge through a narrow east and west gap. The southwest end of the Vlightberg terminates in steep cliffs over- looking Hasbrouck avenue, to the southwest of which street the land surface is low and hidden under the buildings of Rondout. The western slopes of the Vlightberg and of the North hill, as we will designate that portion of the ridge lying north of Delaware avenue, while locally steep, are not so high and do not present such precipitous bluffs as are seen on the eastern slopes. All along the western side of the Vlightberg ridge is a valley about 14 mile wide, with its bottom at levels varying from 75 to 200 feet A.T., which separates the Vlightberg ridge from the plain on which the city of Kingston is built. The eastern edge of this plain is formed by the Esopus grit, and the Onondaga limestone is ex- posed on it in a series of low anticlinals forming a belt about 3, mile wide. The city of Kingston proper lying still farther west is built on the alluvial plain of the Esopus valley, which, with an elevation of about 175 feet, extends from near Stone- ridge, about 8 miles southwest of Kingston, to Mt Marion, 7 miles north of the city. This plain is underlain by shales of the Marcellus and Hamilton formations deeply buried beneath allu- vial deposits. / Why) HHH } I ate by am} MH gece } VES iff a a » SS <) ol a @ x is) 3 << uv GC wate m 2 a 3 : wo @ ° ba 14 44 44 44 ~“ x r 3 E 0 i zg ° 3 a ° £ + HH I TT Lower Sgluric LEGEND To} 200 500 Scale in feet Map of the small area inclosed in quadrangle shown on plate 1. The Vlightberg includes the area south of Delaware avenue; the North hill, that between Dela- ware avenue and the crossroad near Terry bench mark. REPORT OF THE STATE PALEONTOLOGIST 1902 . ELD Kingston and Rondout are located on the southerly continu- ation of that zone of Appalachian folding to which, in the vicin- ity of Catskill, Professor Davis applied the name of the Little Mountains, and the geologic formations of Siluric and Lower Devonic age are here exposed in more or less parallel folds of northeasterly trend. The particular district in which we are interested, that lying within the small quadrangle on the accom: panying location map [pl. 1], lies at the eastern edge of the Little Mountains along the line of maximum folding, and at the apex of the angle which marks the change of trend of the folds from a southerly to a more southwesterly direction. This fact will be better understood by reference to the geologic map of New York State on which the exposure of the Helderberg lime- stones is shown to bend at Rondout sharply to the southwest through an are of about 25 degrees. This change in the direc- tion of outcrop is not due to erosion only, but is caused in great extent by variation in the directrices of the folds and thrusts, and is related to the presence of numerous interlocking thrust planes of small width which have been observed in the cement mines and in the quarries of the Becraft limestone. . The geologic map [pl. 2] is a sketch map based on part of the Rhinebeck quadrangle of the United States Geological Sur- vey topographic atlas, and is approximately correct. The areal distribution of the formations is-indicated by symbols which are used also in the cross sections. The italic capital letters on the cross sections are explained in the legend of the map. Certain localities to which frequent reference is made in the text are indicated on the map, by letters, as follows. A Gross’s residence on Delaware avenue B Becraft abutting against Oriskany north of Gross’s resi- dence C Cloonan’s quarry on the first Becraft vein, east side of North hill D Delaware avenue quarry E Engine house at north end of Vlightberg G Gross’s quarry in Becraft limestone on Delaware avenue H Hill quarry on Glory hole vein on east side of Vlightberg 1180 NEW YORK STATE MUSEUM J Anticline on Vlightberg near western side Kk Outcrop of Manlius limestone at side of road leading to house on top of Vlightberg | M Middle quarry on Glory hole vein on east side of Vlightberg O Old quarry on Becraft limestone east side of North hill S Spring quarry at junction of Delaware avenue and Yeoman street | T Taylor’s corner quarry at south end of Vlightberg, on Has- brouck av. | | U Unconformity exposed near Taylor’s corner V Vertical cut in Becraft limestone, west side of Vlightberg W White lime quarry on Becraft limestone, east side of North hill , . Generalized section The geologic formations exposed in the Vlightberg and in the North hill range from Champlainic (Lower Siluric) to Ulsterian (Middle Devonic) in age, and their order of sequence and thicknesses are shown in the following table: Feet Onondaga limestone... . . 75 Middle Devonic.....Ulsterian............ Rsopus grit. | 2) So 25 cane ee Oriskanian........... Oriskany sandstone and limestone? 22s eae 60 Rite Port Ewen limestone... . 150+ Lower Devonic..... Helderbergian........Becraft limestone....... 40 New Scotland shale...... 100+ Coeymans limestone... . . 50 Manlius limestone....... 45 Upper Ontaric or . ws Rondout waterlime...... 15 Upper Siluric.....Cayugan.... Sees Cobleskill limestone..... ol ‘* ( Salina waterlime........ 10 Wilbur limestone........ 5—7 Re gape SS Nee Oe ~ Unconformity __ a Leesa Wiebe Ae DP Neochamplainic or Lower Siluric.....Mohawkian.......... Normanskill shale....... 1 000+ STRATIGRAPHY AND PALEONTOLOGY Champlainic The substructure on which lie the Ontaric and Devonic forma- tions of the region is a mass of highly tilted and often much contorted sandstones and shales, usually referred to the “ Hud- son river group,” and probably equivalent to the Normans kill beds of the upper Hudson river valley. In constitution these / “9UOZ poyolmquT oy} Jo ouLTd yey ySoMOT oY} MOTE (FYSII oY} 04) dip AT1oSvoyYNOS B YPM SuIpUy}xe SB UMBIP USE SAVY PTNOYS AA poy{eu ‘spaq ynopuoy oy} g WOTJOeS Uf “STOGYYSITA OY} YSNosy} SMoloos oANJoN.A4G baagsybj py Jo sppiut ybnoayy © T Yolj2ae Jere] vas S253 A > 2 A, 2 55 prossiou 4S wolun 49 [O2UAIA PY o4//bY ‘Yee, if 005 oor ooe ooz oor ° brogybip Jo puaypsou ybnoryy “TT uoyvos noe CE 2787 02S Prosjioy ‘any atomnvysjaT buojo ‘TT 49199S 7 “any avomvsed waanb «BSO4D € 33eId REPORT OF THE STATE PALEONTOLOGIST 1902 1181 rocks are graywackes, or quartz sandstones with argillaceecus cement and with little lime content. In color they are, when fresh, olive gray and, when weathered, dark gray, brown or blackish. They outcrop along the eastern base of the Vlight- berg, have been exposed in some of the underground work- ings specially in the Level and the Middle quarry, and they may be seen to better advantage on Kingston Point, along the right bank of Rondout creek at South Rondout, and in the high hill known as Huzzy hill about 2 miles south of Kingston. Their thickness can nowhere be accurately measured, but it is certainly over 1000 feet. At some points thin layers of black shale are inter- calated in the sandstone, as at the Middle quarry and on Kings- ton point. Some of the heavier layers of sandstone have their surfaces dotted with flattened pebbles of dark shale from 1% to 2 inches in diameter, which appear to have been soft mud when they were deposited there. These sandstones seem to have been largely of shallow water or even of beach origin, for cross bed- ding is common and at some points, notably at the entrance to the Middle quarry, the thinly bedded sandstones with shale part- ings show ripple marks and sun cracks. Fossils are rare. Some thin calcareous layers 1 to 3 inches thick and very difficult to find, contain abundant water-worn individuals of Plectam- - bonites sericea, and Dalmanella testudinaria; and a few graptolites have been found in the shale on Kiagston point. The Champlainic sandstones are found, in all cases where the contact has been exposed, to be sharply and distinctly uncon- formable to the overlying limestones of the Upper Ontaric ’ (Silurian), as described below. Ontaric or Upper Siluric Only the upper members comprising the Cayugan series of the Ontaric system are represented in the Rondout section; the lower members, including the Niagaran and Oswegan series, are absent and their time periods are indicated by marked un- conformity between the upper Ontaric limestones and the subja- cent Champlainic sandstones. The Ontaric formations may be grouped under three heads; the upper Manlius limestone; the 1182 NEW YORK STATE MUSEUM middle cement series, comprising the Rondout, Cobleskill and Salina waterlimestone; and the lowermost Wilbur limestone. These formations are exposed along the steep eastern slopes of the Vlightberg and North hill where they are found dipping at high angles into the hills to the northwest; and some portions of the series, specially the Manlius limestones, are exposed above the overthrust on the North hill, and also below the Vlightberg overthrust plane along the road running to the top of the Vlight- berg at the point marked K on the map. | Wilbur limestone This lowest member of the upper Ontaric limestone series lies unconformably on the eroded edges of the tilted Champlainic sandstones. It is a dark colored argillaceous limestone 5 to 7 feet thick, which on weathering turns brown. In places it is highly fossiliferous, containing corals, crinoid fragments, brachi- opods, mollusks and some trilobites. The fauna of this lime- stone, which has long been known as the “ coralline” and which has recently been termed Wilbur limestone, is described in Mr Hartnagel’s paper in another part of this volume, and details of the unconformity at the base of the Wilbur beds are | described below [p. 1209]. Cement series, comprising the Salina, Cobleskill and Rondout beds These cement beds have been variousiy called Salina, Water- lime, Manlius, Onondaga etc., and till recently [see Hartnagel’s paper on Preliminary Observations on the Cobleskill (‘“ Coral- line”’) Limestone of New York, p. 1109] no attempt has been made te definitely correlate them with any portion of the Siluric section of western and central New York. They consist of nine distinctly marked layers of limestone aggregating about 32 feet in thickness. | The following detailed section of the strata exposed in the Spring and Delaware avenue quarries where the softer beds have suffered the least amount of crushing, and which shows the relations of the cement beds to each other and to the under and ° overlying formations, may be taken as typical of the Vlight- berg vicinity. The names given to the cement beds are those applied by the miners. ‘qsnayjzeA0 Agrenb out] aYYM PUB sUIpPIZUR UJeJsve SULMOYS ‘soldzenb onuEAv oTVMETE PUB Suidg oy} 48 [IY YON Jo pus YYNos Ysnosyy UOloos Ssor) SESE Te = jeaj 005 oom 0€ ©0% +00) ° GEE = s 0/4 fEN4Y4149NO Jo pue 4yinos py» | aonerals buss ybnosyy* WT voyag — —_ [20a] VIS WN = Im Ti ewer ———— ——__— ‘Ay d40mDjag REPORT OF THH STATH PALEONTOLOGIST 1902 1183 Detailed section of the formations exposed in the Spring and Delaware avenue quarries (Stations 301 and 325) 25 Shaly limestone........... 4’,0” 24 Shaly limestone........... 11/,6” Helderbergian...... Coeymans 50’,7”....23 Cherty limestone.......... IgE = | spades, 22 Cherty limestone.......... LAY, OF | _ .38%/a21 Hard limestone........... £08 ical 20 Basal, marly, transition.... 4’,10” 19 Hard dove, massive....... 6/,4” 18 Light gray compact....... ; 17 Stromatopora, upper bed.. 7’,6” Manlius 42’.........16 Stromatopora, bottom..... 5/,5” 15 Dark blue with gray seams. 5’,8” Are Darke bles 3:6 07 oe a. ft 3,10" lide? Phin-bandedi ie. 24425 2). 20g Gayiigan............ 12S Gray an dine 4.) ciats b ccsveh 3 4’ 6” 11 Paving block ormud crack. 37,3” 10 Prismatic or five point..... 4’,4” Rondout 19’,6”...... 9 Leperditia bed............ yp es 8 Curly, variable............ 87-19” @ “Sottgray cement. fs... 3,3” G Hard gray cement, ./.2. 41° 5,07 Gobleskall 5 50.4 3.25 ba, Middle ledae:ie.3e0 02. sie he 5 ‘Hard black cement........ 4’ 8” Salina 9’, 7”-11',2” 4 Soft black cement......... Al bn oe VRB othedtess arc oe 5 6 6”—2’,0” Rar 5/7 oe cee Do) Copal nme eats ania eae a —77.0" oo 2 We OmikOnninl Gy tk OES sod fGen Peet oe Upper Champlainic. .Mohawkian........ 1 Normanskill sandstone... 1000’+ The Champlainic sandstones and the Wilbur limestone are not well shown in this section. Salina Comprising the dark cemerts 3 The “footledge,” of hard, fine grained, almost black lime- stone, varies from 6 to 24 inches in thickness. The upper 6 or 8 inches are of exceptionally fine grain and are used for cement. The lower portion is rough and fossiliferous containing crinoid fragments and Tentaculites which are best seen when the stone happens to have gone through the kilns. 4 Soft black cement. A solid bed, 4 feet 5 inches thick, of dark limestone of finer grain than 3, and with some fossils in middle portion. 1184 NEW YORK STATE MUSEUM © Hard black cement, 4 feet 8 inches thick, is much like 4, but it is somewhat harder, breaks with a more conchoidal fracture, and it often has irregular dark blotches on an olive-gray ground. Cobleskill 5a The middle ledge is a 7 inch band of somewhat shaly slightly more calcareous limestone that can usually be separated from the top of the hard black cement as a distinct bed. This _ band is highly fossiliferous, but the fossils can scarcely be seen in the fresh rock, and they appear best after the rock has been burned in the kilas. A large species of Leperditia is abundant, and Orthothetes hydraulicus and Rhynchonella lamellata are present. This middle ledge of the Vlightberg is, aS demonstrated by Hartnagel, the attenuated eastern exten- sion of the Cobleskill limestone of the Schoharie section. Rondout beds Comprising the ight cements 6 Hard gray cement, 5 feet thick, is a solid bed which on cross section shows horizontal bands of olive-green on a lighter gray ground. The rock has a splintery fracture; is of very fine grain at top and center, and at bottom is quite coarse. 7 Soft gray cement, 3 feet 3 inches thick, has a more even tone of slightly darker gray than 6, and is of finer grain and more conchoidal fracture. : | 8 The “curly” is a 19 inch band of dark gray, fine grain cement rock with undulating lamination, which is usually much sheared and crushed to a dark powdery mass by lateral move- ment of the overlying formations. It is to be noted that in general the lower part of each cement layer is of coarser grain than the upper part, except in the hard black cement which is a smooth stone throughout. Some quartz sand is found in all the layers excepting the hard black. It occurs in the form of well rounded minute grains of limpid quartz scattered irregularly through the limestone, and from its resemblance -to the wind-blown sand of deserts, it may be consid- ered to have been brought by the wind from some near-by arid - lands which bordered or inclosed the mud flats of Neontaric time. | apace | ‘Aydvasodoy yuoserd oy} poonposd pey UoIso1o o1ofoq pure Suy[NVy 1047" VIeI}s oY} JO UOIpISod oY} O}voIPUT UOT}oes Jo JoUIOD Joddn FYSIE 4e sTOqUTAS YIIM Yoorq oy} PUB oovJANS PUL] OY} GACTB Soul] peop C4 L, ‘T[IY JO epIs qsvo 4V our ysnay} MoTEq Speq Jo Svap pAVMYSOM PUL YSNIY}IOAO SuULMOYS ‘Karenb outly oy AA 78 [MY YON Yonoryy Woryog 4jo04 te el ae a a ee ‘ Or ANN v ee te Lil oe ea ee PNG CORN TR nn ABN RN ERODES BA a } cae Se I YSeGaP | y [onset 3 = Se pe ee ee k ey YL fftano | ; 2 Sreaute puo Atson& auUssryz azignn | = pee: DE PEPE SES = Spe apt ES Sa oy fe BY sss SSS So SS AI ZI PI] ybnosy |] ‘AL uolf{Iag ee = — SI 25255 “1% 052 4N0FR-I/BIG [2097 22aS uiojd Puog obopuoug Ae OY, sis Ze SoA Zs Fg AAA: SF GOLZZZ: BAe eee) era ee ee oy ee ma i a tees ne ee ae eee Py -y SET ---7 ¢ 33e%Id REPORT OF THE STATE PALEONTOLOGIST 1902 1185 9 The Leperditia bed, about 25 inches thick, forms the roof in most of the underground cement workings. It is a persistent band of tough black shaly limestone, and is full of the shells of Leperditia alta, which show plainly on the gray weath- ered surfaces of the thin layers into which this formation splits. The Leperditia bed is well exposed in the hanging wall of the several quarries on the Glory hole vein along the eastern slope of the Vlightberg, and also at the old. cement opening on the hill- side over the White lime quarry on the North hill. At the latter point the following species were obtained: Leperditia alta (aa), Beyrichia sp.? (aa) Modiolopsis dubius Hall, and Spirifer vanuxemi. 10,11 Above the Leperditia bed are two bands of yellowish limestone, aggregating 7 feet, 7 inches in thickness, which break up into polygonal blocks [see pl. 6] formed apparently by shrink- age cracks similar to those seen in drying mud, and this resem- blance is rendered more striking by the concave plates into which the blocks readily split along planes parallel to the stratifica- tion. Local names are given to different portions of these two beds, which might perhaps more properly be considered as a single formation. The lower 22 inches is called the “streaked ” because of its horizontal dark lines; the “ prismatic” or “ five point,” 32 inches thick, breaks up into mostly pentagonal blocks 4 to 6 inches in diameter; the “ paving block” or “mud crack,” 15 inches thick, breaks into larger polygonal blocks of 6 to 10 inches diameter; and an uppermost 24 inch layer consists of gray weathering impure silicious limestone. Portions of these two beds make good cement but as a rule they are not quarried because the rock above them does not form a safe hanging wall or roof. | Manlius limestone Beds 12-19 The Manlius limestone, aggregating about 42 feet in thick- ness, consists of eight beds of generally black or bluish gray limestone, with many intercalated thin beds that weather to a light gray. The lower beds, 12 to 16, contain the species so characteristic of the Manlius fauna: Leperditia alta, 1186 NEW YORK STATE MUSEUM Spirifer, vanuxemi; and Stropheedonta’ vara: striata. A few of the gray weathering bands just below and just above the Stromatopora bed contain a gastropod fauna. Bed 17, with a thickness of 7 feet, 6 inches, is a veritable coral reef, consisting almost entirely of species of Stromatopora, which are found also more sparingly in the underlying bed, 16. The ASSO- ciation between the gastropod fauna and the coral reef is note- worthy. The uppermost layer of the Manlius, 19, is a heavy bed of fine grained, dove-colored silicious limestone, 6 feet, 4 in- ches thick, and is apparently barren of fossils. It forms the lowest bed of the Delaware avenue quarry. The upper surface of this dove limestone is curiously irregular and its contact with — the dark overlying basal member of the Coeymans limestone is very sharp. There appears some evidence that the surface of the Manlius was slightly eroded before the Coeymans was deposited on it. Where exposed to the weather for a short time the black limestone can be readily separated from the dove-colored rock and the contact is then seen to be of very undulating nature, as if the soft calcareous mud of the Manlius had been eroded by the currents of the transgressing Coeymans sea when the latter advanced on the sinking mud fiats or lagoons of the Manlius continental shelf. ? FAUNA OF THE MANLIUS LIMESTONES a=abundant aa=very abundant c=common r=rare rr=very rare Gastropod layer just below the Stromatopora bed. Loxonema fitchi Hall, c Holopea elongata Hall Holopea pervetusta (Conrad), ¢ Laevidentalium sp.? H. subconica Hall, ¢ Spirifer vanuxemi Hall, r Loxonema sp.? Leperditia alta Conrad, ¢ Murchisonia minuta Hall Holopea antiqua (Vanuxem) Hormotoma, small species Zaphrentis sp.? Modiolopsis dubia Hall Gastropod layer just above the Stromatopora bed. Spirifer vanuxemi Hall, ¢c Ostracods, numerous specimens of two - Tentaculites gyracanthus (Haton), ¢ or three small species Stropheodonta varistriata Conrad, c Hormotoma, small species Leperditia alta Conrad, c Holopea elongata Hall CTT osed o0s uoNdOSsep 10g “soBJANS ot4 JO jolfor oy} O4Vorput orngord oy} Jo Zoey OY} 4B Sour] OY pu ‘Spoq SuISUYIOAO OY} 4e dn SuLyoo], MOTEq WOT] Usye} ST MOTA ayy, ‘loAV] JUSTO OY} UI SYoRsO pNut TISSO] SuLMOYS ‘peq jyuouUTeD ,,o1yvuIsd ,, pue poq eIZIpsode'] Jo soowjins Jopus) 9 948d REPORT OF THE STATE PALEONTOLOGIST 1902 1187 Dark limestone beds of upper and lower part of Manlius. The fauna of these beds of similar sediments seems both below and above the Stromatopora bed to be the same. Leperditia alta Conrad, a _| Loxonema sp.? Spirifer vanuxemi Hall, a Tlionia sinuata Hall, r Stropheodonta varistriata Conrad, c Devonic formations The Devonic formations exposed in the Vlightberg and on the North hill are of the Helderbergian, Oriskanian and Ulsterian series, ranging from the Coeymans limestone on the east to the Esopus grit on the west side of the ridge. The Onondaga linie- stone is not found on these ridges, but is exposed farther to the westward on the edge of the Kingston plain. Coeymans limestone A series of heavy beds of dark gray limestone, aggregating about 49 or 50 feet in thickness, is exposed along the crest of the bluff on the east side of the Vlightberg and North hill, and also forms a ridge of some prominence above the White lime quarry overthrust, which may be traced through the woods from the vicinity of Gross’s quarry to beyond Terry bench mark. The entire series is seen to best advantage in the Delaware avenue quarry where can also be seen the abrupt lower contact with the Manlius and the gradual upward transition into the overlying more shaly New Scotland beds. The component parts of the Coeymans limestone are as follows, in ascending order. 20) basal bed. 58 inches of irregular, marly limestone of dark gray color, which on weathering readily breaks up into small nodu- lar pieces. It is full of fossils; crinoid fragments and brachiopods are common, and Lichenalia specimens of all stages of growth are particularly characteristic of this zone. On weathered joint planes this rock somewhat resembles the Stromatopora bed. The best places to collect fossils from this bed are in the Delaware avenue quarry, and on the first ridge west of the old cement workings above the White lime quarry. 1188 NEW YORK STATE MUSEUM FAUNA Of THE COEYMANS LIMESTONE | 20 Lower basal bed Lichenalia torta Hall, very abundant. Interesting series of growth stages of this bryozoan can be obtained in the limestone back of the White lime quarry. The colony starts as a cornucopialike zoarium, which some- times attains a length of 14 inches before it begins to assume an irregu- larly flabellate form. An adult frond nearly 6 inches in length was ob- tained in the Delaware avenue quarry. Spirifer cyclopterus Hall, c S. concinnus Hall, c S. perlamellosus Hall, r Rhipidomella oblata Hall, c R. oblata emarginata Hall Uncinulus mutabilis Hall, Strophonella punctulifera (Conrad), ¢ S. varistriata (Conrad), c. Both. flat and highly convex varieties Gypidula galeata (Dalman), c. Not so common in this bed as in the over- lying beds. Form very variable, from large weakly plicate to small strongly plicate forms. Also indi- viduals with bifurcating folds Chaetetes sphaericus Hall, c Meristella laevis (Vanuxem), r Rhynchotrema formosum (Hall), r Rhynchospira globosa Hall, r Rhynchospira sp. nov., ¢ Orthothetes woolworthanus Hall, r Spirifer macropleurus (Conrad), r Megambonia sp.? ¢ Strophonella leavenworthana, r Leptaena rhomboidalis (Wilck.), ec. The concentrically corrugate form with a high geniculation, like that figured in Palaeontology of New York, We oy Die 9. tome Atrypa reticularis Zinne, r. Small in- dividuals with regular fine radial ribs Actinopteria textilis (Hall), r Stropheodonta becki Hall, r S. cf. planulata Hall, r Dalmanella subcarinata Hall, r _Favosites helderbergiae Hall, common in very lowermost portion Pholidops sp.? r Rhynchonella semiplicata Conrad, c Bronteus barrandii Hall, r Proetus protuberans Hall, c Dalmanites pleuroptyx (Green), c D. micrurus (Green), r Phacops logani Hall, ¢ Nucleospira sp.? r Cyrtina dalmani Hall, r Orthoceras sp.? r. Annulated type Bryozoa and some ostracods, unidenti- fied. 21 Seven feet of massive dark gray limestone containing fos- sils which are extremely difficult to extract. Lichenalia torta Hall, c Dalmanites micrurus (Green), ¢ Gypidula galeata Dalman, c Actinopteria textilis (Hall), c. Lamellibranch, large, gen. et sp. nov.? 22 Heavy bed of limestone, 11 feet thick, full of large crinoid stems. bands. common. Atrypa reticularis Linne, a Gypidula galeata Dalman, c Hindia fibrosa (Roemer), a — The upper part of this bed has much black chert in thin Atrypa reticularis and the sponge, Hindia, are Favosites helderbergiae Hall, c Uncinulus nucleolatus Hall, c Sponge, gen. et sp.? REPORT OF THE STATE PALEONTOLOGIST 1902 1189 23 A dark limestone in massive bed 12’, 1” thick with chert in the lower 4 feet. Atrypa reticularis Linne, a Fossils are abundant. | Anastrophia verneuilli Hall, r Hindia fibrosa (Roemer), a | Dalmanella perelegans Hall, ¢ Gypidula galeata Dalman, a pauci- | Strophonella punctulifera (Conrad), r plicate form | Gypidula galeata, large form site| coarse bifureating plications 24 At the top of the quarry a layer 11’, 6” thick assumes a more shaly structure and shows fairly well marked cleavage. It forms, together with the next overlying bed, 25, a transition zone from the Coeymans to the New Scotland limestones. It is full of Gypidula and other fossils, as listed. Gypidula galeata Dalman, aa | Orthothetes sp.? Leptaena rhomboidalis (Wilck.), ¢ | Dalmanella perelegans Hall, ¢ Atrypa reticularis Linne, a | Uneinulus nucleolatus Hall Stropheodonta varistriata (Conrad), c | Lichenalia torta Hall Hindia fibrosa (Roemer), ¢ Spirifer octocostatus Hall (?) Leptaenisca concava Hall (?) r Chaetetes sphaericus Hall Rhynchospira globosa Hall, r Strophonella punctulifera (Conrad) Spirifer cyclopterus Hall, r | Rhipidomella, small species 25 Shaly, dark gray, argillaceous limestone with strongly de- veloped slaty cleavage, 4-++feet, thick, showing in the hill slope above the top of the quarry. Lithologically this rock resembles closely the lower portion of the New Scotland beds farther up the hillside. It abounds in fossils, of which the most abundant is Gypidula galeata. It is considered to be the upper- most layer of the Coeymans limestone, aS above this the index fossil, Gypidula, becomes rare or is entirely wanting. no. 3300) Gypidula galeata Dalman, aa Atrypa reticularis Linne, a Uncinulus nucleolatus Hall, ¢ Atrypina imbricata Hall, ec Spirifer perlamellosus Hall Bilobites varica (Conrad), c New Scotland beds (Museum Datimanella perelegans Hall, c Nucleospira ventricosa Hall, r Parazyga deweyi Hall, r Lichenalia torta Hall, r Platyceras sp.? r (Formerly Catskill shaly and Delthyris shaly limestone; also Lower shaly of Davis) The thickness of this formation is given as 100 feet, but this figure is based on estimate only, as exact measurement of the entire formation has not yet been possible. , At no single point 1190 NEW YORK STATE MUSEUM can a continuous section from top to bottom be examined, and the physical characters of the formation are such that it has suffered great deformation, which is manifested in the pro- nounced slaty cleavage, numerous small folds and local thrusts, all of which render determination of its thickness a matter of much difficulty. Portions of the New Scotland beds are exposed at several points. Among the best exposures are those at the south end of the vertical cut on the west side of the Vlightberg ; along the top of the Vlightberg; on the north side of Delaware avenue; between the Delaware avenue quarry and Gross’s lime quarry; in the foot wall of the White lime quarry; and in a low bluff at the west side of the small swale that extends northwestward from the Old quarry. This formation consists of dark gray shaly limestone bands alternating with frequent thin seams of gray semicrystalline limestone. At some points, as on Delaware avenue; sandy shales are present in the middle of the formation. The lower portion has considerable chert, which is often associated, as in the underlying Coeymans, with an abundance of sponges. The upper portion of the New Scot: land graduates by increased thickness of the limestone bands, which contain abundant “scutellae,” into the lower portion of the Becraft limestone. This transition is very gradual and may be well seen in the White lime quarry, in the Old quarry, in the Vertical cut, and in the quarry which follows the out- crop of the Becraft limestone along the face of the hill at the northern end of the West Shore Railroad bridge at Wilbur. Several feet of the upper portion of-the New Scotland beds are so limy, that they might with equal propriety be included with the overlying Becraft limestone, but the line between the two formations has been drawn at a well marked division plane, which indicates a stoppage or temporary change in the sedi- mentation. FAUNA OF THE LOWER NEW SCOTLAND BEDS From the ledge northwest of the Old quarry Orthothetes woolworthanus Hall, aa Chaetetes sphaericus Hall, ¢ Strophonella punctulifera (Conrad), c | Stropheodonta becki Hall, aa Rhipidomella oblata Hall, c Leptaena rhomboidalis (Wilck), aa Crinoid stems, aa Phacops logani Hall, ¢ Isochilina, minute species, aa Dalmanites pleuroptyx (Green), ¢ : a d d REPORT OF THE STATE PALEONTOLOGIST 1902 1191 Spirifer cyclopterus Hall, c | Meristella laevis (Vanuzem), c S. macropleurus (Conrad), c Dalmanella perelegans Hall, ¢ Proetus protuberans Hall, r Spirifer perlamellosus Hall, c Eatonia medialis (Vanuxem), c Hindia fibrosa (Roemer), ¢ Acidaspis tuberculatus (Conrad), r Strophonella sp.? Actinopteria textilis (Hall), c Lichenalia torta Hall, c Platyostoma sp.?, r Atrypina imbricata Hall, ¢ Eatonia peculiaris (Conrad), c FAUNA OF THE MIDDLE NEW SCOTLAND BEDS From Delaware avenue, between the Delaware avenue quarry and Gross’s quarry Leptaena rhomboidalis (Wilck), a Chonetes sp.?, r Orthothetes woolworthanus (Hall) aa | Lichenalia torta Hall, ¢ Strophonella radiata (Vanuxem), aa Chaetetes sphaericus Hall, branching Dalmanella perelegans. Hall, c form, ¢ Anoplotheca concava (Hall), ¢ Platyostoma, 2 species, r \ Acidaspis tuberculatus (Conrad), c Strophonella punctulifera (Conrad), r Spirifer perlamellosus Hall, c Stropheodonta arata Hall, c Dalmanites pleuroptyx (Green), r S. beckii Hall, c Uncinulus vellicatus Hall, r | Rhynchonella bialveata Hall, r Cyrtoceras, small species, rr R. inutilis Hall, r Meristella, sp. indet., r Strophonella cavumbona Hail, ¢ Phacops logani Hall, r Anoplia nucleata Hall, r Eatonia medialis Hall, c Rhipidomella oblata Hall, c Pholidops sp.?, r R. discus Hall, r _Actinopteria textilis (Hall), r Isochilina, small, ¢ FAUNA OF THE UPPER NEW SCOTLAND LIMESTONE From just below the foot wall of the Becraft limestone at the White lime quarry ps Spirifer cyclopterus Hall, aa Gypidula pseudogaleata Hall, r Rhipidomella oblata Hall, c Stropheodonta becki Hall, c Proetus sp.?, rr Aspidocrinus scutelliformis Hall, aa Stropheodonta sp.?, r Atrypa reticularis Linne, ¢ Rhynchonella transversa Hall, aa Orthothetes woolworthanus Hall, c Spirifer concinnus Hall, ¢ Rhynchotrema formosum Hall, a Ostracods, several species, ¢ Meristella sp.?, r Dalmanites pleuroptyx (Green), r Uncinulus campbellanus Hall, ¢ Rensselaeria mutabilis Hall, r Spirifer perlamellosus Hall, r Actinopteria textilis Hall, r Becraft limestone This prominent formation with a thickness of about 40 feet, consists of massive beds of light gray, white and pink semicrys- talline shell limestone of high purity. It is virtually a con- solidated coquina, made up chiefly of fragments of brachiopod shells and crinoids. It is hard and solid and for this reason its 1192 NEW YORK STATE MUSEUM organic remains, which are exceedingly abundant, can be col- lected only with great difficulty. The lower portion of the Becraft is a bluish gray limestone traversed by many thin shale films which intersect the main bedding planes at small angles. The middle portion of the Becraft is a massive bed of hard light gray, white or pink crystalline limestone, 18 to 20 feet thick, made up entirely of organic remains, and running from 94 to 974% of lime carbonate. | It is very homoyeneous throughout and is accordingly one of the most resistant members of the series, and has suffered a smaller amount of deformation; though it is faulted and folded in considerable degree, it has no slaty cleavage. Both the upper and lower portions of the Becraft are of darker color and are traversed by thin shale films. These shale films seem to have afforded lines of weakness along which movements due to lateral compression have taken place, and these portions of the Becraft are accordingly more broken up than is the middle. The lower dark gray Becraft constitutes a series of limestone beds 10+-feet thick which graduate nicely into the thinner layers of limestone forming the subjacent New Scotland beds. There is however a well marked division plane between the two forma- tions. es The upper Becraft, 6-+feet thick, of somewhat darker gray lime- stone, traversed by films of darker shale, anticipates the condi- tions seen in the next overlying formation, the Port Ewen beds, and its upper limit is marked by a prominent division plane. The entire formation is replete with fossils, but the fauna has not yet been well worked out. At a few favorable points fairly good silicified fossils have been collected, but as a rule diagene- sis within the limestone sediments has rendered the organic. remains so indistinct that the majority of them can not be identified. This limestone is of considerable economic importance and has — been largely quarried in this vicinity, as well as to the south- ward and northward from here, for the high grade of lime which it produces when burned. The lighter colored white or pink mid- dle ledge furnishes the best lime. The vertical cut on the west side of the Vlightberg, Gross’s quarry on Delaware avenue, and x a a REPORT OF THE STATE PALEONTOLOGIST 1902 1193 the White lime quarry, Old quarry, and Cloonan’s quarry extend along the strike of the formation northward. There are also extensive quarries in the edge of the Becraft on the hill between Port Ewen station on the West Shore Railroad and the Wilbur bridge over Rondout creek, and the transition from the New Scotland to the Becraft can be well studied on the hillside over the southeast portal of the West Shore tunnel, about 2 miles south from the Vlightberg. ‘e ‘At a few points the Becraft limestone forms ridges of low relief, as is generally the case with such massive pure limestones, but it has as a rule suffered extensive denudation by solution and it occupies the hollows or lies under the lee of protecting ledges of the Port Ewen beds. On the North hill there are two “ veins ” of the Becraft, one in its normal position near the eastern edge of the hill, the second on the overthrust block, running parallel to the first vein and from 700 to 1100 feet west of it. FAUNA OF THE BECRAFT LIMESTONE Middle portion Aspidocrinus scutelliformis Hall, aa U. campbellanus (Hall), aa Spirifer concinnus Hall, aa Stropheodonta becki Hall, a Atrypa reticularis Linne, c Rhynchotrema formosum Hall, r Lichenalia sp.?, ¢ Rhynchonella transversa Hall, c. Meristella sp.?, ¢c | Schizophoria multistriata Hall, ¢ Rhipidomella oblata Hall, c Phacops logani Hall, r Gypidula pseudogaleata Hall, a Stropheodonta cj. varistriata (Con- - Rensselaeria aequiradiata (Conrad), c rad), ¢ Uncinulus nobilis Hall, c FAUNA OF THE UPPER BECRAFT Silicified fossils in clay Gypidula pseudogaleata Hall, a Stropheodonta arata Hall, r Atrypa reticularis Linne, a Leptaena rhomboidalis (Wilck), ¢ Spirifer concinnus Hail, a Nucleospira ventricosa Hall, c Rhipidomella oblata Hall, c Spirifer perlamellosus Hail, c Crinoid fragments, a | Oriskania (?) sp.?, r Port Ewen limestone Above the Becraft limestone is a formation which, because of its influence on the topography of the vicinity, is one of the most important of the series. It was first noted by Davis [1883, p. 39017, who called it the “ Upper Shaly limestone” in contra- distinction to the “ Lower” or “ Catskill Shaly limestone,” now ‘ See Works mentioned in the text, p. 1227. 1194 NEW YORK STATE MUSEUM the New Scotland beds. Davis does not cite any particular lo- cality where this formation can be seen, but this map [op. cit. p. 891] shows the formation, as understood by him, to be present. in all continuous sections in the vicinity of the Vlightberg, the North hill, the Port Ewen section, and in what he calls ‘ the southwestern synclinal,”’ which extends southward for about 2 miles from the village of Wilbur along the western side of Ron- dout creek. Darton [1894, p. 803, 818, map and sections on pl. 4, p. 319-25] describes the occurrence and relations of this forma- tion in the vicinity of Rondout and southward toward Rosendale. At a later date, with the object of eliminating physical terms of nomenclature, Clarke and Schuchert [1899, p. 878] applied the name “ Kingston beds” to this formation, and cited as typical the section seen along the West Shore Railroad southeast of the high bridge over the Rondout creek about 114 miles south of the Kingston depot, which had been examined by van Ingen and - Ruedemann [Clarke, 1900, p. 73]. The term “ Kingston” was however preoccupied and accordingly Clarke [1902, p. 666] sug- gests the name Port Ewen, taking it from the name of the West Shore station near which the formation is seen to best advantage. The Port Ewen beds lie between. the Becraft limestone and the Oriskany sandstone and they consist of massive beds of impure siliceo-argillaceous limestones which slightly resemble the New Scotland limestones that lie below the Becraft. The minimum thickness, aS determined by careful measurements at different points in the vicinity of Rondout, varies from 110 to 160 feet, and the formation probably attains, in places, a maximum thick- ness of about 200 feet. The peculiar characteristics of these Port Ewen beds are best seen in the cuts along the West Shere Railroad between Port Ewen station and the southeast end of the high bridge at Wilbur, and in the prospect tunnel driven into the hanging wall of the White lime quarry on the North hill. Other favorable points for examining the formation are: on the hill- — ‘side over the southeast end of the West Shore Railroad tunnel at Wilbur, where the entire formation is seen lying between the Becraft below and the Oriskany above; on the top of the quarry in the Becraft limestone along the curved outcrop of the syn- clinal trough southwest of the Port Ewen railway cut; in the REPORT OF THE STATE PALEONTOLOGIST 1902 1195 hillside on the north side of Delaware avenue between Gross’s residence and Gross’s quarry; and in the vicinity of Whiteport on the Walkill Valley Railroad, about 5 miles south of Kings- ton. Two sections can be seen at Whiteport: one near the rail- way station shows the Port Ewen beds underlying the Oriskany sandstone; the other section in the biuff on the east side of the track about 1 mile south of Whiteport station, shows the Port Ewen beds, 180 feet thick, outcropping at the top of the bluff between the Becraft and Oriskany. The fresh rock of this formation can best be obtained in the prospect tunnel of the White lime quarry, which with a length of 152 feet has penetrated a thickness of 107 feet of the Port Ewen beds without reaching the chert near the top of the forma- tion. It is hard dark gray, evenly fine grained siliceo-argillace- ous limestone of very uneven fracture, containing a considerable amount of finely disseminated iron pyrites, which hastens the decomposition of the rock. One of the most characteristic fea- tures of this formation and one which renders it easily recog- nizable from a distance, and which is best observed in the rail ~ way cuts and on the hillside near the tunnel at the Wilbur bridge, is the presence throughout the greater part of the forma- tion of well marked concretionary nodules of purer limestone, which lie in lines parallel to the bedding planes of the rock. The fresh rock of the nodules is slightly lighter in color and it weathers by solution of its lime content much more rapidly than does the general mass of the formation. The residual material is a yellowish brown sandy mud rock or “rotten stone” which is easily carried off during rain storms, so that lines of cavities are formed in the exposed edges of the formation. These pock- ets of rotten stone often contain well preserved silicified fossils. With exception of the lowermost portion of the formation, which, through a thickness of 10 or 12 feet just above the Becraft, consists of lighter colored, more fossiliferous, purer limestone, the general mass of the Port Ewen beds is not prolific of organic | remains. They can not be obtained at all from the fresh rock (except in the basal layers), but careful search of the weathered surfaces and specially of the rotten stone pockets, will yield a considerable amount of satisfactory material in the form of 1196 NEW YORK STATE MUSEUM molds and casts. Such material formed the basis of the list of Species given by Clarke in his description of the section along the West Shore tracks near Port Ewen station [1900, p. 73]. A certain superficial resemblance exists between the Port — Ewen and the New Scotland beds, and as this resemblance may lead, and indeed has led, to confusion on the part of students and others who make hurried visits to the region, it may be well to describe some of the characters by which the two forma- tions may be distinguished. The New Scotland beds are alternating series of bands of shale and limestone, with lines or seams of nodular chert in the lower portion, and the entire series is replete with organic remains. The basal New Scotland is a shaly, blue gray limestone, abound- ing in the shells of Gy pidula galeata. The upper portion of the New Scotland gradually changes from a dark gray shaly limestone to a bluish gray limestone, and finally merges into the heavy beds of the Becraft through gradual increase in the thick- ness of the purer limestone seams and a corresponding diminu- tion of the shale content of the mass. The Port Ewen beds, on ‘the other hand, commence with an impure limestone, without chert, little different from the upper part of the Becraft, which by increase in frequency and thickness of the undulating seams of yellowish shaly material, and corresponding loss or diminu- tion of the lime seams, assumes within 20 feet above the top of the Becraft the typical character of the Port Ewen beds. This typical character is that of massive dark gray, impure limestone that weathers brown and that contains lines of nodules of purer ~ limestone which form cavities in the weathered rock surfaces. Toward the top of the Port Ewen beds the rock changes from the even grained dark limestone, which persists through a thick- ness of about 100 feet, and seams of black chert become intercal- cated in the layers of limestone. These chert layers increase in ~ thickness, the limestone diminishes in thickness, and finally lay- ers of pebbles appear to indicate the proximity of the overlying Oriskany sandstone. The chert layers, aggregating 11 feet, 3 _ inches, in the Port Ewen section, and of slightly greater thick- ness toward the south near Whiteport, seem to mark the upper part of the Port Ewen beds at all points where this formation Ss er eee ee REPORT OF THE STATE PALEONTOLOGIST 1902 1197 has been observed... The lowermost beds of black chert at the base of the Oriskany seen in the east bank of Esopus creek just below the iron bridge where the Mt Marion to Glasco turnpike crosses the creek below Glenerie, about 7 miles north of Kings- ton, are considered to represent the chert beds of the upper part of the Port Ewen formation, though the characteristic Port Ewen limestone beds have not yet been recognized in the vicinity of Glenerie. Another point of difference between the New Scot- land and the Port Ewen is relative scarcity of fossils of the latter formation. Both Davis and Darton emphasize the prominence of the slaty cleavage of the “ Upper Shaly” beds. Our observations in various parts of the region have demonstrated that cleavage is far more prominently developed in the New Scotland than in the Port Ewen beds. This would be expected as the New Scotland limestones and shales are much the softer and less resistant beds. The fauna of the Port Ewen beds is strictly Helderbergian in its expression, no true Oriskany species have yet been found in it, though many of its members are also found in the Oriskany fauna. The list published by Clarke [1900, p. 73] contains the names of species found in the various layers of the formation exposed in the Port Ewen railroad cut. New material obtained from the lower part of the formation along the edge of the hang- ing wall of the White lime quarry affords the following list of species. FAUNA OF THE LOWERMOST PORT EWEN BEDS 7 In edge of hanging wall of White lime quarry This horizon is the same as that of bed 4 of the railroad cut section published by Clarke [1900, p. 73]. Leptaena rhomboidalis (Wilck), c _ Uncinulus campbellanus (fail), ¢ Atrypa reticularis Linne, a. Some Nucleospira elegans Hall, r very old individuals with thickened | Phacops logani HgJl, ¢ anterior margins of shell | Chaetetes sp.?, ¢ Strophonella leavenworthana Hall, c | Hindia fibrosa (Roemer), ¢ Dalmanella perelegans Hall, c Tentaculites elongatus Hall, c Orthothetes woolworthanus (Hall), c Anastrophia cf. verneuilli (Hail) Spirifer perlamellosus Hall, c Spirifer concinnus Hall, ¢ Rhipidomella oblata Hall, ¢ Acidaspis tuberculatus Hall, ¢ Meristella laevis (Vanuzem), c 1198 NEW YORK STATE MUSEUM Oriskany beds The Oriskany of this vicinity presents two distinct kinds of deposits. The lower portion is a pebble bed or conglomerate 6 to 18 feet thick; the upper portion, 26 to 50 feet in thickness, consists of layers of sandy limestones intercalated with bands of cherty limestone, both of which are replete with fossils. The difference petween the typical Port Ewen and the pebbly Oriskany is very great though the change from the one formation to the other’ was not violent, as indicated by the following de- tailed section measured on the West Shore Railroad cut about 14 mile south of the Wilbur bridge. The beds are numbered in ascending order. Feet — Inches _ 14-21 Typical Port Ewen nodular limestone.... 66 2 22 Band) of black chert: (2.02 Aces. ance eee 1 6 23 Impure limestone with much chert in thin . bands; no ' fossilsi. 0.2. fe a ie Bea 9 24 Black, banded chert with thin limy bands. The limestone bands contain a small amount of GUarte Sad oo ue ahah whee ee ae Sea 5 0 25a Layer of quartz pebbles of size of peas..... 0 3 25D ‘Black*: Ghert: (6 aco ee es ae oh ee ee 0) 9 26 Alternating thin bands of pebbles and chert. 3 if 2¢ White: pebble bed esos... 3 2 eee 5 0 A solid bed of well rounded, waterworn, white quartz pebbles, of size varying from peas to white beans, stained with brown iron oxid, ce- mented by limestone in some parts, elsewhere no cement and pebbles loose. Fossils consist- ing of waterworn fragments of the larger Oris- kany brachiopods and gastropods. 20 Black pebble. hed: 209 nae aie Seger: 9 0 This is a sokid bed of white rounded quartz pebbles of about the same size as those of bed 27, but in places attaining even 1 inch in diameter. These are embedded in a tough hard matrix of dark siliceous mud cement, that often assumes the character - of black chert. Among the quartz pebbles are often pebbles of black chert like that of beds 22, 24, 25b; and a few masses of REPORT OF THE STATE PALEONTOLOGIST 1902 1199 concretionary appearance consist of white quartz pebbles in black chert cement. The cement matrix is rarely calcareous, so that this rock resists erosion and decomposition better than other members of the series. Throughout the bed are scattered, sometimes abundantly, much waterworn fragments of Oriskany shells. 29-34 Sharp on the top of the black pebble bed lies a series of siliceous and sandy limestones in thin layers of 4 to 12 inches thickness, which when fresh are very hard and of black or dark gray color, but which when weathered turn into a soft brown rotten stone. These beds with a thickness of 42 feet in this section, constitute the highly fossiliferous Oriskany which has yielded such finely preserved silicified fossils, and of which the upper layers are absent in this section. The entire thickness of this upper portion of the formation approximates 50 feet, in this immediate vicinity. North of Rondout the thickness of the Oriskany diminishes to about 20 feet at Glenerie. Darton’s figures of the thickness of this formation [1894, p. 497] can not be depended on. In the Rondout region, where Darton says it is “30 feet, including the conglomeratic member,” we find it to be at least 60 feet, with the upper portion removed by erosion. A carefully measured section of the Oriskany, including the pebble bed at the base, but without the top layers which here also have been removed by erosion, along the railway at Whiteport station, shows 70 feet, 6 inches of this formation, while Darton [op. cit., p. 497] states “In the Whiteport region and southward the formation con- Sists of a silicious limestone bed which has a thickness of frum 8 to 9 feet.” On the top of the hill 1 mile south of White- port station, the total thickness of the Oriskany is about 80 feet. Ries, in his Report on the Geology of Orange County N. Y. (N: Y. State Geol. 15th An. Rep’t. 1897. 1:402), gives the Oris- kany in the vicinity of the Neversink valley north of Port Jervis a thickness of 125 feet. This thickness increases to the south- ward, as noted by Weller [1903, Geological Survey of New Jer- sey, Report on Paleontology, 3:98] who quotes 170 feet for the Oriskany in the Walpack ridge a few miles south of Port Jervis. The Oriskany of New Jersey contains a fauna, that of the 1200 NEW YORK STATE MUSEUM Dalmanites dentatus zone, which is apparently older than any so far recognized in the Oriskany of New York. This “dentatus fauna ” comprises, according to Weller, in addition to a number of Lower Helderberg species and species peculiar to itself, the following Oriskany types: Stropheodonta magnifica, Spirifer murehisoni; Cyrtinawaoe Strata and Orbiculoidea ampia. It seems to occupy a horizon corresponding to the upper part, possibly to the black cherts, of the Port Ewen beds of the Rondout and Whiteport sections. The limit between the Port Ewen and the otiacine has been drawn by us at the bottom of layer 27, the white pebble bed which marks the commencement of new and peculiar conditions of sedimentation and life of Oriskany time. That the pebble beds owe their origin to currents of considerable strength seems evident from the nature of the fragments of which they are com- posed. The pebbles themselves are in all respects small copies of the rolled white quartz pebbles that compose the massive Shawangunk grit, and their source is perhaps to be sought for in masses of this latter formation, which, during that early Devonic time, projected above sea level in the vicinity of what are now the Shawangunk mountains along the eastern shore of the mediterranean basin or trough in which the Helderbergian and Oriskanian sediments were being deposited. No unconformity can be distinguished between the Port Ewen and Oriskany, though small rolled fragments referable to the Port Ewen black chert occur frequently in the Oriskany beds. : The Oriskany pebble beds are well exposed in the small ridge just west of Gross’s residence; farther to the north they are seen along the western slope of the North hill where they are overlain by the upper sandy and cherty limestones of the same formation. Another excellent exposure, where the loose gravellike character of the lower pebble bed is well shown, is along Abeel street that runs from Rondout south along the left bank of the Ron- dout creek at a point near the old coal docks and about 144 mile north of the South Rondout ferry. The pebble beds are quite constant throughout the southern part of the Little Mountain belt, and they are recorded by Davis REPORT OF THE STATE PALEONTOLOGIST 1902 1201 and Darton as occurring, with diminishing thickness, to the northward as far as Catskill creek. No such clear quartz sand- stone as that of the classical Oriskany localities of Union Springs, Oriskany Falls and Schoharie, has yet been found in the Little Mountain belt. To the southward the pebble beds have been noted as far as Rosendale, and there is no evidence that they do not extend beyond that point. They are not, how- ever, mentioned by Ries from Orange county, and in Weller’s Walpack ridge section in New Jersey, there is a hiatus at the horizon where they might be expected to occur. The upper sandy and cherty beds of the Oriskany are filled ‘with fossils, and at many points, specially where the beds have slightly inclined attitudes permitting the surface waters con- taining vegetable acids to seep through the joint cracks and dissolve the calcareous cement, pockets of residual sandy mud contain abundant, exquisitely preserved, silicified fossils, that rival and often surpass the noted specimens from Cumberland | ‘Md. The best collecting grounds for this material are: in the West Shore Railroad cut between Port Ewen and the Wilbur bridge; on the Waikill Valley Railroad at Whiteport ; along the western slope of the North hill at Rondout, beginning a short distance north of Gross’s house and extending to and. beyond Terry triangulation station. But by far the best locality and one from which in the past the senior author has obtained large and fine collections (now in the possession of Dr John M. Clarke of Albany, and Prof. H. S. Williams of Yale University) is along the right bank of Esopus creek between the Glenerie lead mills and the iron bridge on the Mt Marion to Glasco road. This locality is about 7 miles north of Kingston, and 114 miles east of Mt Marion station on the West Shore Railroad. Here the beds are exposed, dipping about 15° to the westward, in broad areas along the roadside and the bank of the creek, and search in the decomposed material along the joint cracks has brought to light a wealth of fossils, in a state of preservation unequaled elsewhere in New York State. The fauna obtained there, of which an incomplete list is given, comprises upward of 125 species, a large number for a single bed at a single locality. 1202 NEW YORK STATE MUSEUM Several of the species mentioned in the Glenerie list have been found in the various other localities about Rondout, but no record has been made of them. | This Glenerie fauna is quite as large as that of the Becraft mountain Oriskany, described by Clarke [1900], but differs from it in some important respects, of which the most notable is the . larger proportion of New Scotland species present in the Glen- erie beds. No comparison can yet be made between the pelecy- pods and bryozoans of the two faunas, as these organisms in the Glenerie collections have not been identified. The large percentage of New Scotland species (26 out of a total of 94) in the Glenerie Oriskany emphasizes the close affin- ities between the Helderbergian and Oriskanian faunas. Indeed the Glenerie fauna and the beds containing it present essentially a recurrence of the conditions of sedimentation and of the fauna of the New Scotland beds during Oriskany time. The true Oriskany element of the Glenerie fauna (represented by such species as Edriocrinus sacculus, Rhipidomella musculosa, Leptaena ventricosa, Leptostro- phia magnifica and. L.> macniventer., 7? beep. parionyx proximus, the large Camarotoechias, Spirifer arenosus and S. murchisoni, Rens- selaeria ovoides, Megalanteris ovalis, Beachia Suessana, Actinopteria arenaria, etc.) is con- sidered by us to have been derived by migration from a contem- poranecus fauna which cctupied an adjoining basin or trough farther to the westward, under somewhat different bionomic con- ditions. Instead of considering the eastern calcareous beds as Lower and the western arenaceous beds of the Hipparionyx fauna as Upper Oriskany, as suggested by Schuchert, we are disposed to follow Clarke in regarding these twe types as presenting two distinct contemporaneous facies of the Oriskany. At no point have these two facies with their distinct faunas been found Superimposed in a single section, nor have they been found in close proximity to each other. We do not include in this sug- gestion of contemporaneity the Oriskany-Onondaga fauna of Ontario, Canada, which is undoubtedly of later age. The pres- | REPORT OF THE STATE PALEONTOLOGIST 1902 ~ 1203 ence of the genus Ambocoelia, and of the fish spine, Mach- aeracanthus sulcatus, both Devonian types, in the Glenerie fauna is noteworthy in this connection. GLENERIE ORISKANY FAUNA a=abundant c=common r=rare Species marked (N) are New Scotland species; (O) are typical Oriskany species of central New York province; (D) are Onon- daga limestone types. (C) indicates Cumberland Md., species. Chaetetes sphaericus Hall, (N), a Aulopora sp.? Pleurodictyum lenticulare Hall, (N), r Hindia fibrosa Roemer, (N), r— Edriocrinus sacculus Hall, (O), ¢ Fenestella sp.? Orbieculoidea jervensis Barrett, r Pholidops terminalis Hall, (C), a P. ovata Hall, (N), ¢ Rhipidomella oblata Hall, (N), ¢ R. emarginata Hall,- (Lower Helder- berg, Cumberland Md.), r R. musculosa Hall, (O) (C), a R. discus Hall, (N), r Dalmanella perelegans Hall, (N), ¢ D. planoconvexa Hall, (N), a Leptaena rhomboidalis Wilckens, (N),r L. ventricosa Hall, (O), a Brachyprion schuchertanum Clarke, ¢ B. majus Clarke, c Leptostrophia becki Hall, (N), c L. magnifica Hall, (O), a L. magniventer Hall, (O), a L. oriskania Clarke, c Stropheodonta lincklaeni Hall, (O), r Orthothetes becraftensis Clarke, a O. woolworthanus Hail, (N), c Hipparionyx proximus Vanuzem, (O), ¢ Chonostrophia complanata Hall, (O), ¢ Chonetes hudsonicus Clarke, c Anoplia nucleata Hall, (O), a Anastrophia verneuilli Hall, (N), r Camarotoechia pliopleura Hall, (O), c C. fitchiana Hail, (O), ¢ C. oblata Hall, (O), a C. multistriata Hall, r Eatonia peculiaris Conrad, (O), a EK. singularis Hall, (N), r E. whitfieldi Hall, (C), r EK. medialis Hall, (N), r Coelospira dichotoma Hall, (C), a C. concava Hall (1867), (O), ¢ Leptocoelia flabellites Conrad, (O), a L. acutiplicata Conrad, (D), ¢ Cyrtina rostrata Hall, (O), a C. dalmani Hall, (N), r Spirifer arenosus Conrad, (O), ¢ S. murchisoni Castelnau, (O), a S. tribulis Hall, (C), a S. cyclopterus Hall, (N), a S. saffordi Hall, a 'S. modestus Hall, (C), ¢ Metaplasia pyxidata Hall, (O), ¢ Ambocoelia sp. nov., ¢ Meristella lentiformis Clarke, c M. lata Hall, (O), c M. vascularia Clarke, r Nucleospira ventricosa Hall, (N), ¢ N. elegans Hall, (N), r Trematospira multistriata Hall, (N), r T. costata Hall, (N), r T. sp. nov., large Parazyga deweyi Hall, (N), ¢ Rhynchotrema formosum Hall, (N), r Oriskania navicella Hall & Clarke, c O. sinuata Clarke, r Cryptonella fausta Clarke, r Megalanteris ovalis Hall, (O), c Beachia suessana Hall, (C), ¢ Rensselaeria ovoides Eaton, (O), ¢ Pterinopecten proteus Clarke Actinopteria arenaria Hall, (OQ), ¢ Aviculopecten rectirostra Hall, (O), r Megambonia crenistria Clarke, r Spirorbis assimilis Clarke, r Tentaculites elongatus Hall, (O), ¢ Cyrtolites expansus Hall, (O), r C. sp. nov., r 1204 NEW YORK STATE MUSEUM Diaphorostoma desmatum Clarke, c Ostracoda, several minute species D. ventricosum Conrad, (N), a unident. Strophostylus expansus Conrad, (O) ? Cirripede, of Balanoid type Orthonychia tortuosa Hall, (O) Phacops logani Hall, (N), r/ Platyceras gebhardi Hall, (C), ¢ Dalmanites pleuroptyx Green, (N), ¢ P. nodosum Conrad, (O), a D. stemmatus Clarke, c P. reflexum Hail, (C), ¢ Homalonotus major Whitfield, r P. pernodosum sp. nov.,r ona sulcatus Newberry, P. platystomum Hall, (N),r Ee (D), vig fi eas P. lamellosum Hail, (N), r raises padi Sree anuxem (D),e Orthoceras sp.?, r Esopus grit This thick formation cevers large areas of country to the west of the Vlightberg and the North hill at Rondout, and it forms the crests of most of the hills along the roads leading from Kingston . southwest to Rosendale. Its thickness is 300 to 325 feet. Itisa heavy bedded, soft, argillaceous grit of dark olive-brown color and of remarkably even grain throughout its mass, and it is quite barren of organic remains. It has well developed slaty cleavage, which often obscures the deposition planes of the rock, and on its weathered surfaces it breaks down into rounded hil- locks covered with*small angular fragments of the stone. Its lower beds are quite heavy, somewhat harder in texture, and their bedding planes are covered with the fucoid Spirophy- ton caudagalli Vanuxem. | The formation can be well seen in the high bluffs overlooking the left bank of the Rondout creek just north of the Wilbur bridge, and also in the cuts of the West Shore Railroad between the Wilbur tunnel and the Wiltwyck cemetery. It is also finely exposed in the left bank of the Esopus creek at Glenerie its type locality. Its upper layers become more limy and finally, through grad- ual changes they merge into the argillaceous limestones of the lower portion of the Onondaga beds. This transition can be well seen in the West Shore Railroad cuts south of Kingston station, and in the banks of Esopus creek beneath the West Shore bridge at the Glenerie falls. The only fossils found in this formation are Leptocoelia acutiplicata, Atrypa spinosa, an obscure Disci- noid brachiopod and Spirophyton caudagalli. REPORT OF THE STATE PALEONTOLOGIST 1902 1205 Onondaga limestone This formation is not found on either the Vlightberg or North hill, but as it is one of the most important members of the series in the Kingston region, a few words are devoted to its character- istics. The upper part of the Esopus grit merges into the lower _ portion of the Onondaga by such gradual changes that no line of demarcation can be drawn. These lower impure limestones are about 40 feet in thickness, and they are overlain by about 380 feet of purer blue gray, hard silicious limestone that lies in beds of from 1 to 5 feet thick. The upper portion of the pure limestone carries considerable black chert that projects as irregular knobs on the weathered surfaces of the rock. This formation abounds in fossils, but the rock is so hard and splintery that they are very tincule to extract. Atrypa reticularis, Lepto- strophia perplana, Platyceras dumosum, Leptaena rhomboidalis, are the most common species. The Onondaga limestone is well exposed along the West Shore Railroad between the Wiltwyck cemetery and the tunnel; several quarries have been opened into it within the Kingston city limits; and it is also finely exposed along the western slope of the mono- clinal ridge that parallels the east side of the West Shore Railroad for several miles north of Kingston, specially in the vicinities of Lake Katrine, Glenerie falls, Mt Marion and Saugerties. ; Range of the Helderbergian and Oriskanian species The following table shows the range of the various species of fossil organisms throughout the members of the Helderbergian and Oriskanian series in the Rondout region. The table is based on the lists already given in the text above; and Clarke’s list of the Port Ewen fauna, published in his Becraft memoir [1900, p.73], has been incorporated. The relative abundance of the species is indicated by letters: a=abundant, c=common, et are, V— present. Hipparionyx proximus Vanuzem...|. Chonostrophia complanata Hall... . Chonetes hudsonicus Clarke........!. 1206 NEW YORK STATE MUSEUM ue) ae ele 8% BE ala 2 od es 2 o/e BE of Oo o o SL SS ee ae Be br Se as) is) SS eee Hindia fibrosa Roemer....:........ Ame gic Sponge, gen. el Sp.0) so 1 a. ces fe Sits ag ete Auloporasp. ie Gil sae te Sipe eae he Feat ec cee Chaetetes sphaericus Hall ......... c Wat sCi 26 CASp 3EP ROE RE EL ee oe re Duncanella rudis Garty............ eae Favosites helderbergiae Hall....... Cae Pleurodictyum lenticulare Hall.....|. Zaphrentis roemeri EL. & H.........|.. ae Aspidocrinus scutelliformis Hall... .|.. a Edriocrinus sacculus Hall.......... oe Kenestella spite. rake ne oe aka: SCAR Pan Lichenalia; torta tall... j. 4k. -te se a Cyr SC MC Te SDs te nea ace 6 [a cine ene eee Se Cladopora smicra Clarke.......... ie Orbiculoidea jervensis Barrett...... ae Pholidops ovatus Hall ts. 2... .... ae P.terminalisiiailss «2668 a. Bae ee a ze Phholidops) spe tsa s .0 aoe ee 18 me r Bilobites varicus Conrad.......... EEL ek kee Dalmanella perelegans Hall....:...|.. ¢@¢ | ¢ € ; D, planoconvexa alls. ©. 22s) ii. me ve D. subcarmata Hal: ace ater r 7 Rhipidomella discus Hall.......... = rf Rvemareinata alls: 3752 hae ae Vv R.museulosa, Halls, 2226 oa) aoa a ae ie Ry oblate stale: 2e x. CA hee Cc eae c Ries Samal, SPPCCHES'.r:-6 hag ee eee eee ns c Schizophoria multistriata Hall ..... fe tae Pacers Leptaena rhomboidalis Wilck...... c CS ana ik; venbricosa diall. che fae. Nop ileae a Leptaenisca concava Hall ?........ j r i Stropheodonta arata Hall...... ye Bre (CN ae S. beck Wall aowhi ale ees Se oe BLE GC Sy limeldlaeniay alls Va AR elas cee nace ae Stropheodonta cj. planulata Hall...| r ee S). varistriata Conrad:. ...4<. .s8 hs € c Stropheodonta cj. varistriata Conrad). . Brachyprion schuchertanum Clarke... B. majus Clarke....... SFE ery SE * Leptostrophia magnifica Hall...... ; LL. maeniventer Jiall: ss ian ares L oriskami anlage oe 9) te Seca Ste ni uk Strophonella cavumbona Hall..:..:.!.. c S:deavenworthana Hole! xa eee VaR Sa gee ae S. punctulifera Conrad.........:.. Herr Nes Aeneas S; radiata Vane.) sy oy ae oaes m Beat | Straphonellaispy tics ihe sti meee erase Wei. Orthothetes becraftensis Clarke.... .. ; Sea Bie O. woolworthanus Hall.......... ah eck Al Tea Bee OSD aac eed pte ae ame Rn ee ae a r Lower Becraft Middle Becraft Upper Becraft do: Lower Port Ewen r) Upper Port Ewen Oriskany at Rondout Jae QnteH. Oriskany at Glenerie fe qo: *. OOpPand-: QQ oO = Se ae j Q is) a | Esopus grit oo aoe ee eee ee ee imal Sas REPORT OF THE STATE PALEONTOLOGIST 1902 aq 4 Ss BE g 8 5 oO Ss KS Hs Be SAE iicy (a Anoplia nucleata Hall.............|.. ies Gypidula galeata Dalman ......... ec ¢ yb PRB WERE, av eia cleo ee ec c G. pseudogaleata Hall............. Eee Anastrophia verneuili Hall.........).. r Rhynchonella bialveata Hall.......).. .. Peeembtlig Fall... ee ee es poRes 4S R. semiplicata Conrad............. ee Peemamoverss, Halas oss eee sues laos ore Uncinulus campbellanus Hall......).. .. Me mtnbtlis Hall... ccc. iiss she ess cain Mine mmmai ION sc cae vase ee hec aa me moelcolatus Hall... 2... eee es |e c ‘Uncinulus vellicatus Hall..........).. Se Rhynchospira formosum Hall...... ene Camarotoechia fitchana Hall........|.. raministrtate GU 6. coe wie «since los =: UTE 1 er Poa sperates, Phe ar sh Gemmopleura Hallo. eee lee ae © parrandyfall......... Tee eo a a ea Eatonia medialis Vanurem........|.. _ E. peculiaris Conrad...... fSkavereiae Sh: Pepmemiaris Hal. ok ee eee ee lee ePwibOeN OL. fe. cee ek hes Spirifer arenosus Conrad..........|.. os 00 Lt i 3 0) a re Cra Beevclopterus Hall... 50. e. es Geth, S. macropleurus Conrad........... eae S. modestus Hall....... Ppa tothe tate eh S. murchisoni Castelnau............|.. Spirifer cj. octocostatus Hall .......|.. .. Segecamellosus. Hall 00... es one is ae S63 TULUM 5 1 Age a ee Ie Seats ION. oo sk Me ee we be Yd Cyrtina dalmani Hall............. boa OSD US Wee ls (01 el ara areal Ambococlia spi NeP.: oe... 6 os des Metaplasia pyxidata Hall..........].. Trematospira costata Hall.........).. Pemegiistata Hall. 2.5 i... en ess Meese 700. 1AToe eke ees ek che we Rhynchospira globosa Hall........ Don Ly SOT me Areas Gru Parazyga deweyi Hall.............1.. Nucleospira elegans Hall...........].. ie wenuricosa, fall. os. oe lee MGC OSPITAS P2605. Liv uw be ds bee Tr Atrypa reticularis Linne...........| r a PeeOS TH. ae weal eo 8 oy Atrypina imbricata Hall........... =a Anoplotheca acutiplicata Haill...... =e premconeava Hall::....... 6%. en es ie Peemaneiites FGI, oo. oo. oie wk eae ws se Coelospira dichotoma Hall.........).. Upper Coeymans Lower New Scotland Cc Cc ee 5 aa ae We We: e4) Poles = hes Bike. ec | ¢ Middle New Scotland Lr ar | 1207 : - | ;o -~ © a a ais 8 ee le AR h Be n| es % aml S| B/E g Bie e/3 2/4 Ae Ae lea, ee eles S| Sa 8/5 og 8) 2 a; ES e\6 ale ee Plo a PIH PIO Ol ae sdhpettel oi a r SAE heat decane nn BA aeatal | cong URE 2 a Cy walks Re aes Cc APS it aaa a a ae STS ae STAs es Aa ye aA tae ASE ‘ Lees ae Neb Vone hye? See eave are ah - el hid Ne We Le Va c ies: ag By Cea seed a Shae tcuod VY AWE Mieke EUG ae ni of iheke Meee Rad |kelgepiat at « st Rilo cap sings ver Ie a ee a ee Vi bi ae be ake r Cie Poets c Seal pe ee OS aed . a Sri tae : Lote, © OQ. = + - 1208 NEW YORK STATE MUSEUM Lower Coeymans Middije Coeymans Upper Coeymans Carr SS =a ae Yr M. aie aria Clane By Ce ects coe ents Rensselaeria aequiradiata Conrad...|.. ..-..). R. mutabilis FT OE gy OG ee Neue Megalanteris ovalis Hall. . Oriskania navicella Hall & Clarke.. Oi simuata Clarke. se a te es Oriskamia Spot: cscs lovee ae La Cryptonella fausta Clarke.......... |. Actinopteria arenaria Hall.........|.. aes Ae saberstilis a Ua oa te ioe ate Ter Aviculopecten rectirostra Hall... . Cypricardinia lamellosa Hall.......|.. Lamellibranch gen. & sp. nov.......|.. ries Megambonia crenistria Clarke......|.. Pterinopecten proteus Clarke.......}.. Cyrtolites expansus Hall...........).. CESp OU Sie or ewe ae cee ee lee Diaphorostoma desmatum Clarke. . D. ventricosum Conrad...........[.. Orthonychia tortuosa Hall........|.. Platyceras gebhardi Hall...:......).. iP lanvellosam Falla uae ss ee ee Ps nodosum Cong vary) eee P. pernodosuny sp. 700)... ae Po platystoma Hal eos ee eae P; Bee AUS AE eae Sr Sa er coats i tides PRS Doe ee pee ae ee nee ere een eT reas Strophostylus expansus Conrad.....|.. Spirorbis assimilis Clarke......... ae Tentaculites ones Ba ee Nes Cy TbOceras SiO Spe tn ea ees ee Orthoveras spp miu een’, Sec iat pee tuberculata Conrad......|.. .. Bronteus barrandii Hall........... Tie. Dalmanites micrurus Green........ Mi we D.-pleuroptys Green a ee c DP, stemmatus Clarke.27 054. @. Yh Homalonotus major Whitfield...... we Hi, vanuxem Wale 2. sueton ee mi Phacops logani Hall..:...... 5... 2. Ch Proetus conradi Hall.......... fe gal: P: protuberans Halleck ae c Proehuss py: Pea ic Maan Can eases ise Machaeracanthus sulcatus Newben "y he Spirophyton caudagalli Vanuzem.. Lower New Scotland ie) Middle New Scotland | Upper New Scotland Upper Becraft Middle Becraft | Lower Becraft 1 ie") | Lower Port Ewen ed: < | Upper Port Ewen J ad<4- -QHHpHOoOdpPatAd. | Oriskany at Rondout ond. | Oriskany at Glenerie | Hsopus grit Gia Hq 5 . REPORT OF THE STATE PALEONTOLOGIST 1902 1209 STRUCTURAL FEATURES The cross sections on plates 3, 4 and 5 portray the large tectonic features of the Vlightberg and North hill. No attempt has been made to illustrate in these sections the smaller folds and faults which are so numerous in all the quarries and mines. - Iilustration of these details is reserved for a future paper. . The term “vein” is employed in the Rondout region in a sense Similar to that in which it is used in the coal regions, namely for a single layer or for a composite series of layers of sedi- mentary rock quarried for economic purposes. It has no rela- tion to and should not be confounded with veins of metallic ore deposits. The compass readiugs here given have all been reduced to true meridian on the basis of 9°30’ west declination for Rondout. The unconformity between the Wilbur limestone and the Champlainic sandstone The Wilbur limestone and the underlying Champlainic sand- stone and shale are sharply unconformable at all points in this vicinity where the contact of the two formations can be observed. It can, however, be seen only along the east side of the Vlightberg and in the underground Vlightberg mines. The nature of this unconformity has been well described by Davis;1 and we can add only a few details to his description. The sur- face of the tilted sandstones at the unconformity, a surface which represents a very ancient plane (probably Eosiluric) of subaerial degradation, is much more uneven at some points than at others. At the locality marked U near the south end of the Vlightberg, where the unconformity was studied by Davis, and where our photograph [pl. 7] was taken to show the same view illustrated by Davis’s sketch [1883. p.392], the eroded edges of the sandstone form a very irregular surface with hollows 6 to 24 inches deep. These hollows are in the nature of grooves parallel to the bedding planes of the rock, and the largest grooves coincide with the most prominent de- position planes, the latter having furnished lines of least resist- ance for the eroding agent. The hollows are filled with the “T1883. p. 392-93; and 1890. p. 355. 1210 NEW YORK STATE MUSEUM Wilbur limestone, and in the limestone have been found rounded waterworn boulders of sandstone incrusted with fossil bryozoans and corals. . Farther to the northward, at the Hill quarry, the old land surface of the sandstone is quite smooth, but still farther north, in the incline into the North quarry just west of the engine house (I on map, pl. 2), the same surface is again as rough as at the first locality. The unconformity is expressed not alone by the eroded sur- face of the Champlainic sandstones, but also by the discordant | strikes and dips of the involved formations, which lie at nearly right angles to each other. At the locality U the sandstone strikes n. 10° w. (true meridian) with an easterly dip of 60°; and the Wilbur limestone strikes n. 55° e.; dip 30° n. w. This general attitude of the two formations is maintained at all- points where the unconformity has been measured, though there is some variation in the relationship, which can be ex- plained by supposing the dip and strike of the sandstone to have been somewhat variable when the region was submerged beneath the Siluric waters of the Wilbur sea. At the angle of Union street, just south of locality U, the sandstone strikes n. 21° w., dip 60° e. On the old tram track below the Middle quarry, the sandstone strikes n. 24° w., dip 70° e.; and the Wilbur in the hill above strikes n. 49° e., dip 75° w. At the entrance to the Hill quarry, which is an excellent place to examine the un- conformity, the sandstone strikes n. 44° w., dip 50° n.e.; and the limestone strikes n. 41° e., dip 75° n. w. On the incline in the North quarry, which is just west of the engine house (marked E on map, pl. 2), the sandstone strikes n. 4° to 6° w., dip 70° e.; and the limestone strikes n. 71° e., dip 10° w The nonconformity represents a period of land conditions in _ this vicinity which continued through the epochs of deposition of the Shawangunk grit, the Medina sandstone, the Clinton lime- — stone and shale, and the Rochester shale and possibly the Loek- port limestone. All of these formations, absent from the hon- -dout section, were laid down farther to the westward and south- ward, as described by Hartnagel in his paper on the Cobleskill limestone. G0Z1 esed 900 «= 4S¥OyLOU SHOOT MOIA ‘[Z 1d] deur oy) uo FQ poyarvM quiod oy} 38 S1oqyySITA 943 Jo pus YyNOos oy} AvoU ‘SoUOyspuUvS dIUIe[dWIRYD oY} puv VUOJSOUMTT] ANQTIAA EY} Jo Ayrur1oJUOOUL-) REPORT OF THE STATE PALEONTOLOGIST 1902 1211 Structure of the Vlightberg The principal structural features seen in the Vlightberg are a monocline and two anticlines, all of northeasterly trend, and a small overthrust block. 1 The Glory Hole vein along the east slope of the hill, is at present a monocline of steep northwesterly dip, though it may have originated as the eastern limb of a compressed or faulted synclinal trough. 2 An eastern anticlinal arch, just northwest of the Glory Hole vein, is seen at the surface at the Delaware avenue quarry at the northeast, in the underground workings of the Spring, Level, and Middle quarries, and again is exposed at the surface in the small arch just east of the Taylor’s corner workings at the south end of the Vlightberg. 3 A second, western, anticlinal arch forms the _ north- western half of the Vlightberg. The axis of this arch passes. through the point J, and just west of the point K on the map [pl. 2], and its western limb is exposed in the steeply dipping Vertical cut along the outcrop of the Becraft limestone [see V-V, map, pl. 2]. | 4 An overthrust block of small extent and uncertain relation- ships, cut off by the fault 2-2 at the north end of the Vlightberg. 1 Glory Hole vein The most important feature of the eastern side of the Vlight- berg is the long deep cut made in the Glory Hole vein of the cement rocks, which extends with a general strike of n. 60° to 70° e. from the engine house (EK) southwestward for about 600 yards to beyond the Middle quarry (M), where it loses its identity. . This “vein” of cement rock has an outcrop at least 20 feet wide that appears on the hillside at altitudes varying from 100 feet at the engine house to about 175 feet between the Hill and the Middle quarries. The vein dips into the hill at the steep angle of 75° to the northwest, and at the northeast end, be- tween the engine house and the Hill quarry, it has been exca- vated in the Glory Hole workings to a depth greater than 150 feet below tide level. In these deeper workings, and also in 1212 NEW YORK STATD MUSEUM the shallower workings along the vein near the Hill quarry and north of the Middle quarry, the same trend of n. 60° to 70° e., and dip of 75° n. w., are maintained with remarkable regularity in the foot wall of the vein. On the other hand, the trend and dip of the hanging wall of this vein are not so constant and they vary greatly in the vicinity of local disturbances of the cement beds. Toward the south side of the Middle quarry the Glory Hole vein assumes a flatter position, and at the point U, which is near its southernmost outcrop, its dip is 30° n. w. and its atnike . 5B° e eee at certain points, as at about halfway between the engine house and Hill quarry, shown in the distance of the photograph [pl. 8], the Glory Hole vein is a simple vein about 20 feet thick, there are other sections where the vein has been duplicated and even tripled by diagonal strike faults, the planes of which intersect the vein at small angles, generally 10° to 20°. Such diagonal strike faults, which are in all cases thrusts of small displacement with the upthrow or thrust on the north- west side, are best seen at the north end of the Glory Hole cut [pl. 8 and 9], at the Middle quarry [fig. 2, pl. 12], and at the Hill quarry. At one point near the south end of the deeper workings of the Glory Hole vein, such a diagonal fault brings up a wedge of Wilbur limestone, the angular crest of which rises — toward the southwest. Following the Glory Hole vein through the Middle quarry toward the south end of the Vlightberg, we find that its dip decreases, and that it is split by a diagonal strike thrust fault, with upthrow on the northwest side, into two veins, which south of the Middle quarry give rise to two sharp though small ridges now capped on their northwestern slopes by Wilbur lime- stone, and showing Champlainic sandstones on their southeast- ern slopes [see pl. 12, fig. 2, 83, 4]. The right hand ridge, with a strike of n. 55° e., on which is the finely exposed section of the unconformity at locality U [pl. 7], is the continuation of the Glory Hole vein, which has veered somewhat to the southeast ~ and which here has a northwesterly dip of only 30°. The second — Plate 8 The Glory Hole cut, looking southwest from the corner of the engine house. The foot wall at the left is Wilbur limestone; the hanging wall is the Leperditia bed. The snow covered mass in foreground 1 is top of a pier. REPORT OF THE STATE PALEONTOLOGIST 1902 1213 ridge, designated “vein B,” [pl. 12, fig. 3 and 4], with a strike of n. 60° e., dip 30° n. w., appears first as a small wedge-shaped block in the south side of the Middle quarry, the block increas- ing in size and hight to the southwest till it becomes of the same prominence as that bearing the original vein. The north- westerly dipping Wilbur limestone on the western surface of this “vein B” block is broken in the trough at the bottom of the slope by a small fault, which separates it from the south- easterly dipping Wilbur limestone that covers the eastern limb of the anticline of the Taylor’s corner vein. This small fault coincides with the axis of a synclinal fold, which, though here broken, had a complete trough, now eroded, at no great distance to the southwest. Northeastwardly the amount of displace- ment along the fault plane increases rapidly, and at the Hill and Level quarries the two broken edges of the cement forma- tions are widely separated, how far is as yet undeterminable. At any rate this fault affords a clue to the puzzling relations of the Glory Hole vein and the eastern anticline. fe 2 The eastern anticline At the southern end of the Vlightberg the Taylor’s corner vein of cement [pl. 12, fig. 3 and 4] is bent up into a sharp anti- clinal fold of northeasterly trend, the crest of which is distin- guished in the rounded ridge, covered by Wilbur limestone, that extends northeastward from the old Taylor’s corner engine house. The southern end of this anticline is cut off by erosion, and a good section of it can be seen along the southeast-north- west portion of Union street [pl. 12, fig. 4]. The eastern limb of the anticline is very narrow at this point, as it extends only to the fault in the bottom of the first trough east of its crest, a dis- tance of perhaps 40 feet. The western limb is of much greater width, and, with a dip of about 45° to the northwest and strike of n. 70° e., it slopes under the high overhanging escarpment of the Manlius and Coeymans limestones. This vein was ex- cavated for a considerable distance underground and it was found to be abruptly truncated along its entire western edge by a small overthrust fault of northwest dip and northeast strike [pl. 12. fig. 3] by which the Champlainic sandstones were 11d . NEW YORK STATE MUSEUM. carried upward toward the southeast to form the hanging wall of the vein along its truncated edge. The amount of displace- ment along this thrust plane has not been determined, as no exploration in search of the missing vein has yet been made. The axis of the eastern anticline dips at a low angle to the northeast, as can best be seen in the northerly portion of the Taylor’s corner workings. The Middle quarry, which is next northeast of the Taylor’s corner quarry, shows a structure quite similar to that of the latter, namely an anticlinal arch dipping slightly to the north- east, its wider western limb dipping steeply to the northwest and finally being truncated by an overthrust fault which brings up the Champlainic sandstones into the hanging wall. The eastern limb of the Middle quarry anticlinal is however some- what different from that of the Taylor’s corner vein. It is wider, and steeper, and, after having been followed in the quar- rying operations for some distance, perhaps 150 feet, on its southeast dip toward the Glory Hole vein, it was found to curve — sharply downward and to diminish in thickness and eventually to dwindle to a knife edge. Still farther northeast on the same anticlinal arch are the Level workings, which present essentially the same features in the form of the vein, with the exception that the anticlinal arch has here a small longitudinal trough on its summit just west of its crest. The barren, much contorted zone lying be-— tween the eastern limb of this anticlinal and the Glory hole vein is crossed by two or three tunnels or crosscuts, and abun- dant evidence of slipping along On ye dipping planes can be found. | The Spring quarry adjoins the Level workings on the north- east. Here also the anticline appears, but with a slight south- westwardly dipping crest, and with its direction changed toward the left to a strike of n. 42° e. This quarry is just north of the apex of the angle that marks the change in the directrices of the folds of this region, as already referred to on page 1179. The apex falls somewhere between the corner of Delaware avenue and the engine house, and in this small area we find structural features seen nowhere else in this region. North end of Glory Hole cut, looking from top of second pillar northeast toward the engine house. Note the folded and faulted gray cement in left side of first pillar, and the striated and scaly thrust plane at the bottom of the Pris- matic cement in the hanging wall. The foot wall is Wilbur limestone. REPORT OF THE STATE PALEONTOLOGIST 1902 1215 The western limb of the anticline has not been explored to a sufficient depth in the Spring quarry to enable us to state defi- nitely what becomes of it, and whether or not it is truncated by a fault in the same manner as are the veins in the other quarries to the south. . There are on the surface of the ground some indications of a fault of northeast trend that crosses Delaware avenue at a point about 400 feet west of where the tram track crosses the avenue at the angle, but the plane of a fault intersecting the surface of the ground at this point would pass’ several hundred feet west of the strike of that deep fault which truncates the veins of the Level and other quarries. The eastern limb of the Spring quarry anticline presents much the same features as shown in the other quarries. On the surface of the ground the anticlinal arch shows finely in the Delaware avenue quarry and in the stripped area west of the shaft house at the Spring quarry incline; and an ex- cellent sectional view of it looking in a southwest direction can be obtained on the flats from the old floor of the Spring quarry ~at the foot of the hill near the junction of Delaware avenue and Crane street. In the Spring quarry face and in the face of the Delaware avenue quarry, which lies above the Spring quarry, a continuous, undisturbed section of the Siluric and Lower Devonic formations as far as the New Scotland beds can be measured. The entire thickness of the Manlius and the under- lying cement beds is shown in the face of the old Spring quarry, and the base of the Coeymans limestone is seen breast high above the floor of the Delaware avenue quarry. On the south- east side the beds dip steeply toward the flats. The crest of the anticline is broad, so that the floor of the quarry is almost flat, and at the quarry face the beds show a slight dip to the northwest at the top of the western limb of the anticline. On the south side of Delaware avenue, between the Spring quarry shaft house and the engine house [pl. 3, sec. 3], is a small knoll of Manlius limestone, the beds of which dip about 30° toward the southeast. This knoll presents a fine example of “imbricated structure,” or “schuppen-structur” induced by several nearly parallel minor thrusts from the southeast. These thrusts are peculiar in that their planes, which are from 1216 NEW YORK STATE MUSEUM 12 to 15 feet apart, converge toward the surface of the ground. Their effect is to produce a quartet outcrop of the Stromatopora bed of the Manlius limestone, and greatly to increase the ap- parent thickness of the latter formation. There has been little crushing along these minor thrust planes, and a shear zone of only: ;, to 1 inch thickness can be distinguished; but, never the- less, the opposing faces of rock have well developed slickenside surfaces. Close faulting with almost no shear zones is on the whole characteristic of the dislocations in the limestones of this region. These minor thrusts are very similar to some of those figured by Sir Archibald Geikie, 1888.1 | The formation of these minor thrusts was probably imme- diately consequent on the plication of the anticlinal arches, and their origin is assigned to torsion forces that buckled the anti- clinal arch. . A most interesting feature of the eastern anticlinal is the pair of approximately parallel tranverse thrust faults of north- easterly dip that transect the anticlinal arch and cut it into three segments. Little trace of these two faults can be distin- guished on the surface of the ground, but they have produced important complications of the underground cement veins. The Taylor’s corner vein, after having been worked out across the entire width of the anticlinal arch, finally dipped toward the northeast, its foot wall flattened, and the farther edge of -the © vein was truncated by a northeasterly dipping thrust fault which afforded a hanging wall of Champlainic sandstone. The southern end of the Middle quarry has a higher elevation than, and actually overlies the broken end of the Taylor’s corner vein, and it, in turn, at its northeastern end dips steeply and is cut off in similar manner ‘by a thrust plane. Beyond this second thrust plane the same vein is being worked at a higher altitude in the south end of the Level workings. These transverse faults are all overthrusts from the northeast, and in conse- _ quence of their presence the segments of the eastern anticline have been “telescoped,” so that they overlap each other after the manner of a vertical row of earthenware tiles on a roof. ae Recent Work of the Geological Survey in the Northwest Highlands of Scot- land. Quar. Jour. Geol. Soc. London. v. 44, fig. 4-21. 5 Ye ON Oe eae Plate 10 Contorted beds over the entrance to Glory Hole incline, just to right of fore- ground of plate 8. Curved bed over entrance is Leperditia inclosing core of Pris- matic. To left of this a wedge of gray cement faulted on itself. The other side of this wedge is shown in plate 9. Upper portion of figure occupied by Leperditia and Prismatic beds. See page 1220 REPORT OF THE STATE PALEONTOLOGIST 1902 LT We have here the only direct evidence seen in this vicinity of the existence of a compressing force acting from the northeast, and even this force may be indirectly due to the same torsion stresses that produced the buckling of the anticlinal arch. It seems appropriate to cite here other phenomena which we consider to have been caused by torsion forces acting after the formation of the main features of the region. Among them are: the virgation of the Glory Hole vein at its southern end; the small diagonal strike thrusts that intersect the hanging wall of the Glory Hole vein, and several similar thrusts seen in the Becraft limestone at the White lime quarry; the diverging minor thrusts of the Becraft limestone in the Vertical cut; and possibly also the small overthrust mass that caps the northern top of the Vlightberg. 3 The western anticline When passing over the Vlightberg along the line of section 1 [pl. 2 and 3] the Coeymans limestone is found faulted on itself over the hanging wall of the Glory Hole vein. This condition is best seen at the Hill quarry where the lower mass of Coey- mans limestone has fallen away from the overthrust plane into the quarry, leaving the deeply striated under surface of the thrust mass finely exposed to view. This thrust mass of Coey- mans, which dips at a high angle (almost 80°) toward the north- west, curves upward toward the top of the hill and becomes in- verted toward the northwest, and finally is lost just below the crest of the cliff along an approximately horizontal crushed zone that marks the presence here of a dispersed fault. Above this crushed zone the Coeymans limestone appears in its normal at- titude exposed in low ledges of northeasterly trend just east of the tenant house on the hilltop. These ledges of Coeymans extend along the entire eastern edge of the hilltop, with an exposure about 50 feet wide, and at a point about midway be- tween the tenant house and the edge of the Middle quarry their strike is n. 50° e., dip 60° n. w. At the southern end of the Vlightberg the strike of the Coey- mans and New Scotland beds veers to the west around the Spooning-up end of the small synclinal trough that occupies the northward-opening swale on the top of the Vlightberg. 1218 NEW YORK STATE MUSEUM Through the point marked J on the map, plate 2, passes the axis of the western anticlinal arch, on the crest of which are exposed ledges of Coeymans limestone that show in the field on top of the hill overlooking the Vertical cut. These Coeymans beds dip slightly toward the northwest. A short distance down the northwestern slope of the hill the New Scotland beds are found, and near the foot of the hill the steeply dipping Becraft limestone has been quarried in the Vertical cut [V-V, pl. 2]. The limestone in the Vertical cut stands nearly on edge, with a strike n. 75° to 80° e., and its apparent thickness is somewhat increased by a virgating series of several minor thrust faults. These faults radiate from an axis parallel to the strike of the - limestone and located a short distance below the floor of the quarry, they cut the bedding planes of the limestone at low angles, and in each case the upward thrust is on the north- west side. | The bowl-shaped area just north of the point J is filled with. drift deposits, so that its substructure can not be determined. 4 The Vlightberg overthrust The western and northern edges of this overthrust plane are marked on the map [pl. 2] by the heavy black line 2-2, and-its position is roughly indicated on section 2 [pl. 3]. On the south side of Delaware avenue, just beyond the shaft house of the Spring quarry incline, there is a knoll showing an anticline of Coeymans limestone, the axis of which points south- westwardly across the fields toward the Vertical cut. The path that crosses the east side of this knoll leads under the cliff of New Scotland limestone on the north side of the Vlightberg and then joins the lane that runs to the tenant.house on the hilltop. On the northwest side of the lane is a field with no outcrops of rock. The lane itself runs over Coeymans limestone which outcrops at intervals, dipping to the east at low angles. Along the left or eastern side of the lane the New Scotland limestone of the low cliffs is very much shattered and dips steeply to the northwest. Continuing on up the lane, the Man- lius limestone, with strike n. 20° e., dip 10° e., appears at the. point K on the map, at the angle of the road where it turns up the hill toward the house. A little farther on, a low escarp- Faulted and folded beds of cement rock and Manlius limestone in face of cliff over the Glory Hole incline. This view is immediately above that shown in plate 10. See page 1220 i REPORT OF THE STATE PALEONTOLOGIST 1902 1219 ment crosses the road diagonally and can be traced for some distance to the right into the field and in the opposite direc- tion toward the northeast into the woods. This escarpment is formed by the upper part of the New Scotland limestone, which has here a strike of n. 60° e., dip 55° n. w., and which marks the- western edge of the overthrust mass. In the woods northeast of the lane a narrow strip of basal Becraft limestone overlies. the New Scotland at the edge of the escarpment, also dipping steeply to the northwest. The contact plane of this overthrust can not be seen along the northwest side of the hill, but its course is plainly indicated by the topographic features, the sharp angulation of the slope,. and the narrow gully which extends for a short distance through the woods along the foot of the slope. On the north and north- east side of the hill the thrust plane can be readily distin- guished, specially in the cliff over the Glory Hole and Level inclines. Here it is seen as a well marked plane cutting diagon- ally across the cement and Manlius beds at about the hight of the peak of the roof of the head-frame shed [thrust 2, pl. 11]. On the eastern slope of the hill, between the engine house and the Hill quarry, this plane seems to rise toward the southwest, and its location is soon lost, probably through dispersion of the fault. This thrust is from the southeast, and it involved in its move- ment only the upper layers of the eastern anticline, and shoved these a short distance along an almost horizontal plane toward the northwest till they rested on the southern limb of the _ western anticline. It seems to belong to the system of minor convergent thrusts, described on page 1215, as imbricating the Manlius limestone in the area north of the engine house. Its position is only a few feet above the uppermost of those thrusts, and its attitude is more nearly horizontal. We see no reason for associating this Vlightberg thrust with the much more ex- tensive White lime quarry overthrust of the North hill, described below. The outcrops of Coeymans and Manlius limestone along the lane probably belong to the southeastern limb of the western. anticlinal arch. 1220 NEW YORK STATE MUSEUM Contorted beds at mouth of Glory Hole Before leaving the discussion of the Vlightberg, we wish to call attention to the complex and highly interesting folding of the rocks over the mouth of the Glory Hole incline [see pl. 8 tu 11]. Of these plates, numbers 8, 10, 11 are adjoining views all looking southwestwardly from the engine house. Plate 8 is from the southeast corner of the engine house, looking along the Glory Hole cut. Plate 10 is a view of the lower portion of ‘the cliff from the platform of the Glory Hole head-frame on the west side of the engine house. Plate 11 shows the upper portion of the cliff as seen from the western edge of the engine house roof, and its lower portion duplicates the upper portion of plate 10. The relations between plates 8 and 10 will be better understood when it is recognized that the small wedge of ce- ment rock in the top of the pillar in the right of plate 8 is the Same wedge that shows to the left of the center of plate 10. It is shown also in the lower left hand corner of plate 11, where it is marked “gray cement,” and a view of its opposite side is seen in plate 9, where it is marked “ H?.” Overhanging the Glory Hole incline is a long closed recum- bent underfold of Leperditia limestone containing a core of Prismatic cement. This fold can be traced along the foot of the cliff toward the right for about 30 feet, till it is lost in the vicinity of the Level incline. To the left of this fold, in the top of the pillar which was left to support this very unstable portion of the Glory Hole hanging wall, are wedges of cement rock, the structure of which is best shown in plate 9. These wedges are remnants of a faulted mass, produced by one of those diagonal strike thrusts described on page 1212, by which the Glory Hole vein was here duplicated to form what the miners call a “double vein.” Above the recumbent fold is seen the edge of a thrust plane [thrust A, pl. 11], that appears to be the continuation of the fault plane which produced the beautifully striated and scaly - surface on the hanging wall of the Glory Hole cut, shown in plates 8 and 9. Next above is a series consisting of Leperditia, Prismatic, Paving block, and lower Manlius (beds 12-14 of sec- tion, p. 1183), which are terminated above by the almost hori- Plate 12 double anticline Level fig. Z: O° but < 90°. The axes make an acute angle and growth takes place in a posteroventral direction. These are the Loxogoniacea and are representd by Venus and a large group of sinupalliate Dimyaria. . 2 a—90°. The axes stand at right angles; growth takes place ventrally, perpendicular to O— A. These are the Orthogoniacea _ represented by Pectunculus. 3 4 > 90° but < 180°. The angle of the axes is obtuse and growth takes place anteroventrally. These are the Prosogoniacea represented by Mesodesma and Nucula. It is to be here noted that this expression is just the reverse of that of the Loxogoniacea the two standing in the relation of left and right valves of Venus. Here as well as in groups 4 and 5 the beaks are truly opisthogyre and current characterization of these valves conse- quently erroneous. — 4 4=180°. Both axes coincide but growth is forward rather than backward as in 8. No examples are known. Noetling be- lieves they should be looked for among paleozoic forms. 5 a > 180° but < 270°. These are the Protoconchae. Growth takes place dorso-orally and the ventral organs and pal- lial line would lie close beneath the umbo. No examples of these were recognized, but it is thought that such forms will be — found among the paleozoic species. — 64 > 270°. These are the Staurogoniacea, raatbemapi amie like group 2 but with growth in the opposite direction, i. e. dor- sally instead of ventrally. No examples are known but these . are also to be sought in the paleozoic. | | T a> 270° but <360°. The axial angle is again acute, the — growth posterodorsal. These are the Opisthogoniacea and em- brace Avicula and the Heteromyaria. | 8a=0° or 360°. That is the axes coincide. These are the Symptogoniacea and are represented by Pecten. Growth is pos- terior. The species are Monomyarian. REPORT OF THE STATE PALEONTOLOGIST 1902 1231 In Noetling’s diagram, of which a copy is given on page 1229, it will be observed that coincident with these varia- tions in the angle of obliquity is the passage from the Dim- yarian into the Monomyarian divisions. This brief statement of Noetling’s determinations should be supplemented by the reader with the perusal of the original paper or the English abstract as cited. In elaborating the genus Lunulicardium which is so exten- sively represented in the Intumescens zone of western New York I have secured some very delicate barite replacements of the valves of Lun. clymeniae which retain the protegulum and give some indications of the value of torsion of the shell as an ontogenic character and it has become possible also to make some observations on the probable phylogenic significance of the same feature. Lunulicardium has been commonly re garded as a bivalve with a long and wide byssal opening. Beus- hausen has shown that the beaks in a certain subdivision of the ’ Fie. 1-4 Umbonal parts of Lunulicardium clymeniae showing triangular area and the attitude of the prodissoconch with reference to the mature shell. The apex of the seers shell is directed obliquely backward and its posterior end is the umbonal point of the adult genus (Chaenocardiola) to which Lun. clymeniae_ be longs are opisthogyre. We have, in a memoir on the Lamelli- branchs of the Intumescens zone in New York, presented a careful analysis of the generic characters but it here suflices to state that the evidence supports the construction of the hiatus between the valves as a byssal orifice while the umbo of the adult shell and the 1232 NEW YORK STATE MUSEUM apex of the prodissoconch are distinctly turned away from the -byssal cleft or backward. With this orientation of the shell the beaks are opisthogyre. ‘The larval shell or prodissoconch lies with its apex or primitive beak directed downward or toward the postlateral extremity of the adult shell, so that the original posterior extremity of the larval shell actually lies at and constitutes the beak of the adult. This relation is shown in the accompanying figures. The shell has in growth actually twisted with reference to the animal and the axial line which we have marked o-a has apparently trav- eled through a large angle to reach the corresponding position in the adult, O-A. The muscula- ture consisted probably of a single adductor corresponding to M on Noetling’s diagram. This expresses itself on the best preserved internal casts as a simple moderately large scar as shown in the figure adjoining of Lun. hemicardioides or it may be an approximation of two central scars as seen in Lun.mtilleri. In the former the condition seems to be the Fic 5 Diagram giving outline of adult © : . Lunulicardium clymeniae with outcome of fusion of the approxXl- larval shell attached: o-a, oro-anal axis in adult shell; o-a the same in young shell; mate scars of the latter. The w, wu, crescence line inthetwo. The lower } are indicates the very large critical angle shell is thus in effect Monomya- for the adult stage, the upper arc, the criti- cal angle for the young stage. The for- . : Se At ay < mer is normal to a position between the rian, though of Dimy arlan 1n- Opisthogoniacea and Symptogoniacea, the Cc epti On. latter in agreement with the critical angle | of He Eromeep acing: In comparing this . wit oetling’s figures it is necessary to If now the shell of Lunuli- bear in mind that here the exterior of the 3 . valve is represented while in that the in- cardium be construed and ori- teriors are given. This will account for the apparent reversal of direction in the ented as a Dimyarian then the two angle between O-A and W (crescence-line) is less than 90° and conforms to this angle in the extreme Dimyarian line. But in such orientation we unavoidably reverse the extremities of the oro-anal axis, the anal extremity, or A, appearing on the byssal side which we know to be a condition not exist- ee oe a REPORT OF THE STATE PALEONTOLOGIST 1902 12350 ing in the lamellibranchs. The inference therefore that Lunuli- cardium has little to do with the Dimyarians is supported by empirical evidence of a single adductor or median approxima- tion or fusion of two adductors. Hence orienting the shell as Monomyarian posited between Avicula (Opisthogoniacea) and Pecten (Symptogoniacea), on the basis of its muscular and byssal structure, we find that the critical angle is exact for the position taken. We take this as excellent confirmatory evidence of the Monomyarian affinity of the genus. Interual fae Eres asaoeiate SRE Ho tee sidnaioe aac SS Se Mae In following the torsion backward from the adult condition to the prodissoconch we find that it passes through the angles neces- sary to bring it with precision to the condition of the Protocon- chae and the relations of the axis in the latter also correspond with those of the prodissoconcht. I believe therefore that the -prodissoconch stage is an actual representative of the Protocen- chae condition and that the stages of torsion of the Lunulicar- dium shell in subsequent growth are indicative of its phylogenic stages of progress toward the Monomyarian stock. This con- clusion is based wholly on external characters and the fact of actual observed torsion in the shell from youth to adulthood. ‘The Protoconchae being theoretically the primitive lamellibranch condition, we may never come to know it except in this or a similar manifestation. The supposed position of the pallial line in this group, just within the hinge, is a feature on which the nature of our material permits no observation. _ + The reader will note that we are here dealing with the exterior of these shells. Noetling’s figures are based on interiors ; hence the relations of the latter and Our figures are reversed. SOME DEVONIC WORMS BY JOHN M. CLARKE Plates 27 and 28 Though trails and tubes of Annelids are of sufficient frequency ‘in Paleozoic rocks to indicate the abundance of these creatures ‘from early Cambric time onward, yet the actual bodies of worms have been so seldom reported that an additional discovery of ‘them seems to justify record. Paleozoic remains believed to be -Annelid bodies of errant worms have been described from the Cincinnatian by Ulrich, and Ruedemann has recently given an -account of certain leechlike worms called Pontobdellopsis from the Utica shale of New York. We have before us a series of specimens taken from the upper Devonic of New York which seem to us correctly interpreted as bodies of Chaetopod worms ‘directly allied to Aphrodite, the well known sea mouse of north Atlantic coasts which we have had abundant opportunity to study ‘in its natural resorts. They have been collected from certain fine grained felspathic argillaceous flagstones belonging to the final phase of Portage sedimentation in the town of Italy, Yates county, and in the Tannery gully at Naples, Ontario county. Of one, whose structure seems rather the more puzzling, there is a number of specimens, of which in two instances we have opposite sides representing dorsal and ventral aspects, which it may be here said are not greatly unlike because the tenuity of the body substance save on the back has made the latter the predominant expression. These are all from the former locality. Hasty examination of these specimens might find in them a suggestive resemblance to the loose, detached rays of short armed ‘Ophiurans. We call attention to this resemblance lest the sapient critic fall into travail at this point. Auother spe- cies is represented by several clearly defined examples from the Naples locality, where it is associated with Parop- sonema cryptophyum and some other unusual species. — The basis of comparison of these with existing Errant Annelids lies in the apparent presence in both of a double series of trans. — verse scuta or hardened overlapping plates on the back. Such -structures are found among living Polychaete worms only in the REPORT OF THE STATE PALEONTOLOGIST 1902 1235 family Aphroditidae and we may here introduce so much of the characterization of these forms as pertains to the interpretation of the objects in hand: W. Blaxland Benham in the Cambridge Natural ee [ve 2, 1896, Polychaet Worms, p. 309] says: The most characteristic feature of this family and one by which its members are absolutely distinguished from all other Chaetopods, is the possession of scales or “elytra” on the back. These flattened dorsal cirri are of a somewhat horny texture and are earried, generally, on alternate seg- ments of the body, filamentous cirri occurring on the other segments. In the subfamilies Peet and Polynoina the elytriferous segments are 2, 4, 5, 7, 9 etc., up to 23; then every third segment. The worms dave Se abhiis short with some thirty- five to forty-five segments, though Sthenelais and a few others have many more. In many cases these elytra are relatively of large size extending backward as broad scutes in two lateral series which may or may not meet and slightly overlap in the middle line. The posterior edge of each scute overlaps that next behind it. In the well known case of Aphrodite, the “ sea-mouse ”, the elytra are covered by a felting of hairlike threads but Her- mione, an allied genus, has them fully exposed. The representatives of both of these genera are short, broad and oval worms. We find no statement as to the alternation of the scutes in these forms except that they are “ arranged as in Polynoe ” where such alternation prevails in most instances. Among the Sigalionina which have longer vermiform bodies “the elytra are in alternate segments up to the twenty-sixth’ and posteriorly on every succeeding segement” [op. cit. p. 313]. Such structures represented by the combination of form and scute-bearing segments we find in our specimens, together with the presence in the case of one species of conspicuous and heavy tufts of marginal setae and in the other sparser hairs plainly arising from extended segmental parapodia. We briefly describe these specimens. 1 Four examples are elongate oval bodies having the outline of a short willow leaf, rather blunt at one end and tapering to a more acute angle at the other. Two of these specimens pre- serve both obverse and reverse of the body and the markings of one side are sharper than on the other; it is evident that they ~ have been impressed from one side to which they properly ap- 1236 NEW YORK STATE MUSEUM pertain, into the other. The more strongly marked or by analogy the dorsal surface carries a narrow median eleva- tion running from the blunt end to near the acute ex- tremity; it becomes continuously more obscure toward this end and may there fail to cause any interruption of the surface. The more complete of these specimens carries about 50, transverse segments, others carry from 40-50 accord- ing to the degree of their completeness. These segmental di- visions are produced by oblique depressions departing from the axial line of the body, bending forward toward the margins but over the median and anterior parts becom- ing more transverse. These depressions bound the surfaces of oblique overlapping plates directed backward or toward the blunt extremity of the body. The plates appear to be continuous across. the full width of the body but are narrowest at the axial line and broader outward, their fore and aft width apparently being at about half the distance between the axis and the outer margin. Their edges are frequently broken off in detachment and the posterior plates appear to be longer and better defined than the others. | Ope These plates (if they are correctly thus interpreted) are rather narrower than similar structures in living species so far as our observation has extended and yet it is not clear to us what part of their actual width has been concealed by their oblique direc- tion into the matrix. The overlap is on the anterior surface of each piate and the projecting posterior edge could not have been greatly extended. Construing the structure thus given from a relief of the natural dorsal mold we note in addition to-the midrib a low submarginal ridge on each side which anteriorly impresses the segments in such a way as to thicken each but posteriorly produces only a sinuosity in the outline of the plates which is doubtiess intensified by the breaking away of the edges of the plates themselves. Besides these there are obscure traces of other longitudinal lines. The posterior extremity of the body is blunt but the anterior end tapers narrowly and in some of the specimens terminates in a smooth blunt subcylindric process which resembles what the head should apparently be in such an organism. ewe eee rere es —s REPORT OF THE STATE PALEONTOLOGIST 1902 1237 Along the lateral margins are broad free fringes like matted bunches of setae which may attain a length of nearly or quite half the width of the body. All the specimens show this char- acter but in one only do these present the aspect of a continuation near the posterior extremity of the edges of the dorsal scutes. One could conceive the thickenings of the margin by the sub- marginal ridges as due to the parapodia. The marginal filaments are usually directed backward, though they may turn forward toward the anterior extremity. The cast of the other, or ventral surface simply presents these various details of structure with some obscurity. These characters seem throughout so suggestive of the features shown by Aphrodite and Polynoe that we shall probably not be far amiss in associating these forms therewith; if not in direct association, at least with the Errant worms. For a designation therefore, we propose to indicate these objects as Pro- tonympha salicifolia. : 2 The second series of these annelids is composed of much more elongate bodies like Phyllodoce or Nereis and are usually curled up in spirals. hese are rather blunt at one end, main- tain a somewhat uniform width for most of their length but taper thence to a narrow extremity. The bodies are distinetly seg- mented, in the best preserved of the specimens there ‘being upward of 100 narrow divisions which are separated from each | other by tolerably deep depressions. In the axial line is a furrow which so divides the segments as to give each the ap- pearance of being in two parts. It is not evident that these segments were plated but the impressions which they leave in sandy sediments seem to indicate this as a possible condition. Kach however bears at each margin a parapodium carrying a bunch of long setae making a fringe often wider than the body itself, and into these parapodia the segments seem to extend without interruption. -The general expression of this structure is very like that of the long row of posterior segments in Chaetop- terus and there is also a notable similitude between the arrange- ment of the segments in the latter and that shown at the broad extremity of the fossil in question, and furthermore in the clear development of the median part represented by the axial line iu 1238) = NEW YORK STATE MUSEUM the fossil body. The single example of these worms which is not closely coiled has the body partly flattened and partly com pressed laterally so as to bring the setae into profile, but the other specimens (three in number) are more or less closely coiled and their structure, save the bristles, is not as distinctly set forth. These all have a certain resemblance to Iulus and other myriapods and the fact of their occurrence in sands where coni- (oii aie = nie a ein ta diel ae, minuted remains of terrestrial vegetation have been freely ac — cumulated, at first suggested this as their probable character. but the specimens do not on close examination reveal the structures of that group. This second group of worms may be | designated as Palaeochaeta devonica. Geoiogic horizon and localities. All these bodies occur in the sands, flags and shales which in the Naples (Ontario county) section lie immediately above the layers which carry the last representatives of the Intumescens fauna. These layers are locally known as the Hatch sands and carry very few fossils, Paropsonemacryptophyum, Orbiculoidea m a g- nifica,‘a linguloid of peculiar aspect, Hydnoceras, with frag- ments of Lepidodendron and other plant remains. With one exception all are from the village of Naples, Ontario co. and Italy hill, 8 miles northeast in Yates county. A single example is from soft olive shales a few feet below the horizon of the Grimes sand- stone, Grimes gully, Naples. OF PLATES 1240 NEW YORK STATE MUSEUM PLATE 1 ° Pentremites leda Hall Page 907 1 The only example of this species observed. x3. Canan- daigua lake, N.Y: Paracyclas lirata Goneia mut. pygmaea nov. Page 910 2, 3 Side and dorsal view. x13. ‘Commdaion, lake, N. y. Nucleospira concinna mut. pygmaea nov. [See pl. 2, fig, 5] Page 904 : “4 Dorsal view of specimen figure 5, plate 2. x15. Greigs ville N. Y. Leda rostellata Hall mut. pygmaea nov. Page 909 5 Dorsal view. x13. Canandaigua lake, N. Y. 6 Left valve. x13. Greigsville N. Y. Nuculites oblongatus Conrad mut. pygmaeus nov. Page 909 7 Cast of left valve. x8. Moscow N. Y. Palaeoneilo plana Hall mut. pygmaea nov. Page 909 : 8, 9 Views of an internal cast. x3. Livonia shaft, N. Y. Nucula corbuliformis Hall mut. pygmaea nov. Page 908 10, 11 Internal cast, dorsal and lateral views. x2. Livonia shaft, N. Y. Palaeoneilo constricta Conrad mut. pygmaea nov. Page 910 : 12, 13 Dorsal and left views of internal cast. x18. Mos- cow N. Y. ete: Nucula lirata Hall mut. pygmaea nov. Page 908 14, 15 Oblique anterior and left lateral views. x13. Livonia shaft, N. Y. Nuculites triqueter Conrad mut. pygmaeus nov. _ Page 909 16, 17 Right and dorsal aspects of an internal cast. x13. . Moscow N. Y. eS eS ee ee ee ee ee ee ee ee PYRITE FAUNA Rep Paleontologist 190c Plate 1. G.S.Barkentin.del. The Argus Co, State Printer. W S.Barkentin. lith. 1242 _ NEW YORK STATH MUSEUM PLATE 2 Grammysia constricta Hall mut. pygmaea nov. Page 910 1, 2 Dorsal and right aspects of a cast. x18. Greigsville N.Y. Nucula varicosa Hall mut. pygmaea nov. Page 908 3, 4 An incomplete cast. x13. Greigsville N. Y. Nucleospira concinna Hall mut. pygmaea nov. [See pl. 1, fig. 4] Page 904 5 An internal cast. x18. Greigsville N. Y. Conocardium eboraceum Hall mut. pygmaeum nov. Page 911 6 Dorsal view. x4. Moscow N. Y. Buchiola retrostriata v. Buch mut. pygmaea nov. Page 911 7 Right valve. x3. Moscow N. Y. Spirifer fimbriatus Conrad mut. pygmaeus nov. Page 901 8, 9 Dorsal and ventral views. x13. Canandaigua lake, N. Y. Strophalosia truncata Hall mut. pygmaea nov. Page 906 10, 12 Dorsal (x5) and ventral (x18) valves. Canandaigua lake, N. Y. | Productella spinulicosta Hall mut. pygmaea nov. - | Page 907 11 Ventral valve. x4. Canandaigua lake, N. Y. Ambocoelia umbonata Conrad mut. pygmaea nov. Page 905 . 13-15 Posterior, dorsal and ventral views. x13. Canan- daigua lake, N. Y. | | Ambocoelia umbonata Conrad mut. pluto nov. 2 Page 905 | 16-18 Ventral, profile and dorsal views. x13. Canandaigua lake, ‘N. Y. | ee a epthageme FAU NA x” 4 PYRIT Plate 2 Dirk flee t 1902 S i Rep Paleontolog W.S.Barkentin., lith. Printer. The Argus Co, Stat G.S.Barkentin.del. Steep 1244 ; NEW YORK STATHB MUSEUM PLATE 3 Spirifer fimbriatus mut. simplicissimus nov. eam 2 Page 901 at’ « 4 1, 2 Dorsal and ventral valves. x13. Canandaigua lake, Neves g Spirifer tullius Conrad mut. belphegor Clarke - Page 903 : 0, 4 Dorsal and ventral views. x8. Canandaigua lake, N. Y. q Spirifer marcyi Hall mut. pygmaeus nov. Page 904 5, 6 Ventral and dorsal views. x8. Moscow and Canan- daigua lake, N. Y. Spirifer granulosus Conrad: mut. pluto Clarke. | Page 903 a 7, 8 Posterior and ventral views. x13. Canandaigua _ 4 lake, N. Y.— : : —- Spirifer medialis Hall mut. pygmaeus nov. Page 902" 4° 2 a a 9, 10 Posterior and ventral views. x13. Canandaigua lake, N. Y. sae Boy | : | Trigeria lepida Hall var. pygmaea nov. 7 . Page 907 é 7 11 Ventral aspect. x13. Canandaigua lake, N. Y. ~ Tropidoleptus carinatus Conrad mut. pygmaeus nov. — oo) Page 906° 4 12 Ventral aspect. x8. Canandaigua lake, N. Y. Spirifer mucronatus Con. mut. hecate Clarke Page 902 ; 138-15 Posterior, dorsal and ventral views. x18. Moscow N. Y. Cyrtina hamiltonensis Hall mut. pygmaea nov. Page 904 ; 16 Dorsal valve. x13. Canandaigua lake, N. Y. | FAUNA PYRITE ith. W.S.Barkentin The Argus Co,,State Printer. ist 1902 G.S.Barkentin.del. fe O a — Ce O, om @) oc ee ye Pokey obarlycia Aiyaw! et tiene Ted oud 1246 NEW YORK STATE MUSEUM PLATE 4 Macrochilina hamiltoniae mut. pygmaea nov. Page 912 »* 1 An internal cast. x18. Moscow N. Y. Diaphorostoma (34 2, 3 Apical and lateral views. x13. Canandaigua lake, N. Y. Macrochilina hebe Hall mut. pygmaea nov. Page 912 4 Lateral view. x18... Moscow N. Y. Pleurotomaria itys Hall (?) mut. pygmaea nov. Page 913 5 Lateral view. x13. Canandaigua lake, N. Y. Pleurotomaria capillaria Conrad mut. pygmaea nov. Page 912 6 Lateral view. xi3. Canandaigua lake, N. Y. Diaphorostoma (?)- 7, 8 Views of shells whose specific relations are uncertain. x25. Canandaigua lake, N. Y. Diaphorostoma lineatum Conrad mut. belial Clarke Page 911 9 Lateral view. x18. Canandaigua lake, N. Y. Loxonema delphicola Hall mut. moloch Clarke . Page 913 i¢ A fragment. x8. Moscow N. Y. Tentaculites gracilistriatus Hall mut. asmodeus Clarke Page 913 11 A view of the shell. x13. Livonia shaft, N. Y. Bactrites? sp. mut. pygmaeus nov. Page 915 12, 13 Two views of an internal cast. x13. Canandaigua — lake, N. Y¥. Orthoceras scintilla Hall (?) mut. mephisto Clarke Page 915 ; i4 Lateral and septal views. Natural size. Canandaigua — lake, N. Y. PYRITE FAUNA Rep Paleontologist 1902. G.S.Barkentin.del. The Argus Co, State Printer. Plate 4 W .S.Barkentin lith. eit : : 1) ~“ BAKE a a 7 a», Cae hate A si st > | ee a hia: So eae NEW YORK STATE MUSEUM PLATE 5 Tornoceras uniangulare Conrad mut. astarte Clarke Page 916 oe 1, 2 Lateral views of two specimens. x13 and x8. Livonia — shaft and Canandaigua lake, N. Y. e Tornoceras uniangulare Conrad Page 916° | 3 Lateral view. x3. Canandaigua lake, N. Y. Bactrites (sp. ?) mut. parvus nov. Page 916 | 4, 5 Lateral and septal views. x3. Canandaigua lake, N. Y. —Orthoceras subulatum Conrad mut. pygmaeum nov. Page 914 6, 7 Lateral and septal views. x13. Canandaigua lake, N. Y. Tentaculites bellulus (?) mut. stebos Clarke Page 914 8 Lateral view of a fragment. x13. Livonia shaft, N. Y. Orthoceras nuntium Hall Page 915 , 9 Lateral view of a specimen. Natural size. Canandaigua lake, N. Y. Eee = Entomis prosephina nov. Page 918 10, 11 Ventral and lateral views. x13. Canandaigua lake, N. Y. Beyrichia dagon Clarke Page 918 12-14 Lateral, dorsal and ventral views. x13. Greigsville N. v4 Cryphaeus boothi var. calliteles Green | Page 917 Ean 15 A fragment of head and thorax. x7. Moscow N. Y. PYRITE FAUNA Rep Paleontologist 190¢ Plate 5 il G.S.Barkentin.del. The Argus €o,State Printer. W.S.Barkentin. lith. ! eraee SF a? tam Ei pe & es t Me Seek . a ne 4! ; ‘ J _ nes #. ° . “ah Ne : 12500 2 . NEW YORK STATE MUSHUM. 97% 149°" * * PLATE 6 : Hughmilleria socialis sp. nov. Page 1091. att 1 Dorsal view of specimen below average size retaining t swimming feet. Shows compound eyes and ocelli. ii " c ee ae 3 i ‘a A Bee ' . ee * Wl ) ed ne va - oA Fe | eis a 4 A “fy yt , i + : . ie as ey CRUSTACEA pie: ontologist 1902. | | Blate 6 ae wort bry. a] : ee _ 2 a = a ae es The Argus Co. State Printers. A.Hoen & Co. lith. als q i ad ee Ae a + 4 ; ; : a , ot ee 5 Ait Ng te a : Ms = ice ep aR i ‘ Pi Rane ate * tag ley : bat et oi cattek™ ‘ 7 kK % ; 4 Sad ‘ 7. . on - e wi 13) eee, NEW YORK STATE MUSEUM ee i A" PLATE 7 3 : : Hughmilleria socialis Sp. nov. oe ne de ee and a one susie wideeraney ocelli and ocelliferous tumescence. Natural size mi a pei CT hy UU aaa wal Mules! as ch f i wt A r ni r A. oy ~ : » uly J - : fi mo 3 CRUSTACEA a «A re VS eq a F ae » i A ‘one 04 is ; x Rep. Paleontologist 1902. Plate 7 3.8. Barkentin, del. "The Argus Co, State Printers. A Hoen&Co.lith. 1254 NEW YORK STATE MUSBUM PLATE 8 Hughimilleria socialis sp. nov. ey, Page 1091 | 1 Ventral view of well preserved specimen. Shows the ex- tended right preoral appendage, three endognathites of the right side (left in drawing) with their coxal joints in position, the mouth, the metastoma, the gnathobases in position, the left swimiing foot, male operculate appendage and the imbricating surface scales. The postlateral extensions of the first postab- dominai ring are also well shown. Natural size ologi st 1902. x The Argus Co. State Printers. _ A.Hoen & Co. th. bar - is * 4 - ~ s a A n 5 ‘ , ‘ ” en Pek, ' Pima? - 4 ‘ o . . ia aS aed re H ~ Y . . : Ne ie i * ; ~ AB * ; * ‘ ; 5 <9 ) on ge { . = =) 1. < ‘ — ’ VP € 1 4 1 e ¢ = > ; ‘ a ; ‘ :. 55 ~ ‘ . 7 - ‘ ; ; De a ‘& re 2 a as ~ = 1 i ey 2 y - ~ ? i 7 2 \ - ed yas > sey ; ' = ie ry - - x c } ” - . ie * mi uke] o er * > t ; a) ove % Key, ? P = a+ ~ ’ - i .‘s a" - ; a ; s . os 4 ‘ { if ove cs ; x . aa + Nokprae ~ ‘ ep ? , ‘ “ : = ‘ as - (ti z % » . + ‘. me r Hee eee i= ns ey Bsa y cars : af) WTAE i & hey ee Sab: na fy oad A es ot aa ay we ny tet & i Be, iS be ye © a uncd. 24 o>: : Lee “ae f ec cha nw Re : mt os Freee ton ab . we en a ws Ba ea + ee ae Pty aac ts 1256 = ————sdNEBW YORK STATE MUSEUM. ~ PLATE 9 Hughmilleria socialis sp. nov. _ [ae Page 1091 | it re a 1 Dorsal view of a large specimen. The anterior portion of * the cephalothorax is broken away and there is thereby expos d ne one extended preoral appendage and the endognathites of the right side. Both swimming feet are also shown. Natural siz CRUSTACEHKA Rep. Paleontologist 1902. Plate 9 G.S. Barkentin, del. The Argus Co. State Printers. A.Hoen & Co. hth. eRe EERE UIT QE aa oe 1258 NEW YORK STATE MUSEUM PLATE 10 Hughmilleria socialis sp. nov. Page 1091 1-6 Cephalothoraces of individuals of various ages, showing slight variations in outline and in the position of compound eyes. Natural size . Eurypterus pittsfordensis sp. nov. Page 1098 7 Upper view of appendages of cephalothorax. Shows the en- dognathites in position, with their clawlike terminal joints, and the gnathobases of the swimming feet. Natural size Hughmilleria socialis sp. nov. Page 1091 8 Two gnathobases of swimming feet. Natural size ) Coxal joint of endognathite. x3 Plate 10 G.S. Barkentin, del. The Argus Co. State Printers. A.Hoen & Co. hth. ial Sha ae 1260 NEW YORK STATE MUSEUM PLATE 11 Hughmilleria socialis sp. nov. . Pages1091 1 Dorsal view of right side of cephalothorax with the four endognathites in position. x8 2 Extended preoral appendage and first two pairs of endo- gnathites. x3 | 3 Pair of preoral appendages, cappecedile in normal position. | x3 4, 5 Preoral appendages showing variations in relative form of the pincers. Figure 4, x4; figure 5, x31, 6 Ventral view of anterior end of cephalothorax, showing the preoral appendages turned back full length, their tips lying over end of metastoma. Natural size és 7 Complete preoral appendage in natural position. x34, : CRUSTACEA Rep. Paleontologist. 1902. A.Hoen& Co. hth. eek eae ie Se Raku oo Beira Aaa CE ah G EON MV Oe ay : FEAST ASG Feria LAR ey OSes eke a hace Rae eR eee aes ~ t a 1262 NEW YORK STATE MUSEUM PLATE 12 Hughmilleria socialis sp. nov.. Page 1091 1 The two posterior endognathites in perfect preservation; and fragments of the two anterior ones. Drawing inverted. x8 2 Anterior portion of cephalothorax showing dehiscence of epistoma through middle and the anterior ends of the gnatho- bases. xBY, 3 Complete swimming foot. x3 : 4 Complete endognathite showing coxal joint, articulation of second joint and lobe of sixth joint. x81, Ps 6, 7 Two metastomata, showing slight variation in form. Nat- ural size a ae SS ee ‘ 8 Section which shows cylindric form of postabdomen. _ Natural size Dolichopterus ? ? ee Ne SO ee ee eee eh, 5 Metastoma of an undetermined form. x3% Plate 12 A.Hoen & Co.h The Argus Co. State Printers. CRUSTACEA st 1902. 1 eee areentin del. Rep. Paleontolog ~e~, Tew ve Are veh 1264 NEW YORK STATE MUSEUM PLATE 13 Hughmilleria socialis sp. nov. Page 1091 1 Middle portion of operculum and second sternite, to show female genital appendages. Shows partial covering of appen- dage of second sternite by opercular appendage. This second appendage should have been drawn:so as to give a more elongate, tubular appearance. x3814 2 Same as preceding, showing appendage of second sternite fully exposed. The longitudinal groove shown on this appendage is the result of pressure against the overlapped edges of the right and left halves of the sternite. x31, 3 View of male operculum and second sternite, showing male opercular appendage. x314 4 Middle portion of operculum and second sternite showing fused parts of female opercular appendage and lanceolate shape of appendage of second sternite seen from inside of body. x2 i, eee ae ees oe a ; CRUSTACEA Rep. Paleontologist 1902. Plate 13 4 See oS SSS = Geer ae G.S. Barkentin, del. The Argus Co. State Printers. A.Hoen & Co. hth. ee ‘ ‘ a, fd i oa *,* —. 1266 © NEW YORK STATE MUSEUM PLATE 14 Hughmilleria socialis sp. nov. Page 1091 1 Male genital appendage, a portion of which is scaled away, giving a cast of the interior. x31, 2 Female genital appendage of second sternite, showing its partial covering by opercular appendage. | x216 - 3 Half operculum with attached female operculate appendage. Naturai size . 4 Half of female operculum showing face of median cleft. Natural size 5) Half of male opereutum showing face of median cleft. Natural size 6 First postabdominal ring segment. Natural size 7 Second tergite showing the anterolateral lobe. Natural size 8 Fragment of seventh joint of Swimming foot, showing group of minute craterlike tumescences. x4 9 First two sternites showing male appendage from the a of body. x2 | iQ Middle portion of fir st two sternites to show female genital appendages, the overlap of the metastoma on the opercular ap- pendage and that of the latter on the next appendage. x2 CRUSTACEA Plate 14 G.S. Barkentin, del. The Argus Co. State Printers. A.Hoen & Co. hth. 1268 NEW YORK STATE MUSEUM PLATE 15 Eurypterus pittsfordensis sp. nov. Page 1098 == 1 Gnathobase. Natural size | : 2. Half of sternite showing transversal suture and cleft 3 Portion of endognathite doubtfully referred to this species, probably fourth endognathite Hughmiilleria socialis sp. nov. Page 1091 cs 4,5 Two views of telsons, showing the dorsal carination. Figure 4, x2; figure 5, x31, 6 Uncompressed telson. x2 CRUSTACEA Plate 15 i ie ee) a ede * gate Pm eal G.S.Barkentin, del. The Argus Co. State Printers. A.Hoen& Co. hth. te _— 1270 NEW YORK STATE MUSEUM PLATE 16 Kurypterus pittsfordensis sp. nov. Page 1098 ; ee 1 Broken cephalothorax and portion of preabdomen showing two endognathites with their coxal joint in position, metastoma and a sternite; and view from the interior of the operculum and male appendage. Natural size CRUSTACEA Plate 16 A.Hoen & Co. hth. The Argus Co. State Printers. G.S.Barkentin, del. 1272 NEW YORK STATE MUSEUM PLATE 17 Eurypterus pittsfordensis sp. nov. Page 1098 | 1 Cephalothorax and first tergite of average specimen showing compound eyes, ocelli and the two triangular scales at base of cephalothorax. Natural size | | 2 Coxa. x4 fe CRUSTACEA Rep. Paleontologist 1902. Plate 17 * Wie tH oy 1274 - NEW YORK STATE MUSEUM PLATE 18 Eurypterus pittsfordensis sp. nov. Page 1098 . 1 Cephalothorax, preabdomen and two postabdominal rings. | Shows eyes, ocelliferous tumescence; scales and surface sculpture of tergites and the posterolateral Jobes of the postabdominal segments. Natural size ; Plate 18 eis, Som Se ee The Argus Co. State Printers. A.Hoen& Co. hth. a) si, ) ie ate aes ae a Ves aren epi ae ee * « ft et ro : = ee ae “SS eee wrt at ~~ ms : , 5 vie Oi ag 4 Sa LP 4s 1276 NEW YORK STATE MUSEUM PLATE 19 Eurypterus pittsfordensis sp. nov. Page 1098 1 Fragmentary abdomen. Shows character of tergites, uo- tably their relative shortness and the fdur triangular scales on each preabdominal and on the first two postabdominal ring segments, while the succeeding two show their ventral characters. The swimming foot is also partially shown. TED size 7" , sry pin » x a rs J R ¥ a h ’ Shae ‘ Plate 19 The Argus Co. State Printers. A.Hoen & Co. hth. ~~ ay "7 . ¥ PP a ‘ 5 . : ‘ re . noe ; Ao SA. f « , y ; . a , . é : . ( Ke . : i - + Fee c y ‘ > 4 . : 3 Liab . Pek ‘ ‘ ~« e ar as . \ , aps ap ‘ ~ > ‘ A : : - i -. 2 : . , a ” > ‘ uy 3] | te “ ie uf Ee, Ly is 3 - . - 4 Nfl a r ¥ - ? ¢ 2 ce: @ , ~ t led & a A * ~ eon r2 Sante EES RIE , . NG r aie . . ie , A " ¢ 4 ie a iy oa : | re = ~ ¥ 5 * 15g a > s ay 7 7 vi z.. . i = ‘ Aisa 4¢'s 1278 NEW YORK STATE MUSEUM PLATE 20 ey Eurypterus pittsfordensis sp. nov. : Page 1098 1 Ventral view of part of last sclerite showing posterior emargination and curved rents. Natural size 2 Dorsal view of last sclerite showing the posterolateral striated spurs and the median denticuiate notch of the posterior edge. Natural size 3 View of two sclerites and telson in approximate positiors. Natural size | ee 4 Ventral view of nearly complete telson. Natural size 5 Ventral view of proximal portion of telson. Natural size 6 Dorsal view of nearly complete telson. Natural size RUSTACEA C Plate. 20 Rep. Paleontologist 1902. A. .Hoen & Co. hth. The Argus Co. State Printers. ne) G.S.Barkentin, del. i ; ni ' 1280 | ‘NEW YORK STATE MUSEUM Bae PLATE 21 Hughmilleria socialis sp. nov. var. robusta var. nov. Page 1097 1 Fragment of carapace showing relatively great width and abrupt postabdominal contraction. Natural size 2 First ring segment showing division of its posterior edge into two lobes. Natural size 3 Incomplete metastoma. Natural size CRUSTACEA Rep. Paleontologist 1902. G.S.Barkentin, del. The Argus Co. State Printers. Plate 21 A.Hoen & Co. hth. 1282S ‘NEW YORK STATE MUSEUM _ PLATE 22, Eurypterus pittsfordensis Sp. nov. Page 1098 1 Fragmentary ventral side of abdomen of ae show’ } joints, ane te ee of suas foot ; fhe five : emargination. Natural size. oe of hope the surface , , | fase CRUSTACKA Rep. Paleontologist 1902. G.S. Barkentin, del. The Argus Co. State Printers. Plate 22 A.Hoen & Co. hth. + SAR i nT, _ > f tin=: A : ta #5 - amy \ ‘ ‘ t » i. = an t . sd A / . ‘ , 1284 NEW YORK STATH MUSEUM PLATE 23 Eurypterus pittsfordensis sp. nov. | Page 1098 . 1 An endognathite referred doubtfully to this species 2 Seventh and eighth joints of swimming foot showing the formation of the slightly expanded blade, the subtriangular inner appendage of the seventh, the incised margin of the eighth joint (palette) and the minute claw inserted on the same. x21 3 Cross section of postabdomen, showing the triangular scales on the tergite. Natural size . 4 Sectien through postabdomen of a very large individual. Natural size CRUSTACEA Rep. Paleontologist 1902. Plateczas G.S.Barkentin, del. The Argus Co. State Printers. A.Hoen & Co. hth. fat wid doh sy Ge ; SE LET SE ae ( ri Mae “ ma $ Tee ai a Pod aay 7 ey en nee ae 1286 = NEW YORK STATE MUSEUM PLATE 24 ‘Hughmilleria socialis sp. nov. Page 1091 1 The free portion of the opercular appendage of a female showing the point of overlap and fusion of the two parts. x2 Eurypterus pittsfordensis sp. nov. . Page 1098 2 Fragment of sternite showing median cleft, transversal suture and lobe of anterclateral angles. Natural size | a 3 Metastoma showing notch and minute dentation of anterior end. Natural size . 4 Coxal joint of fourth endognathite. x21, 5 Female opercular appendage. Natural size Pterygotus sp. Page 1104 6 Fragment of free ramus of chela. x4 Pterygotus monroensis sp. nov. Page 1102 7 Cephalothorax. Natural size Pterygotus sp. Page 1104 8 Metastoma. Natural size Pterygotus monroensis sp. nov. - Page 1102 9 Part of proximal joint of preoral appendage. Natural size CRUSTACEA Rep. Paleontologist 1902. Plate 24 G.S.Barkentin, del. A.Hoen & Co. ith. The Argus Co. State Printers. ie | i238 NEW YORK STATE MUSEUM PLATE 25 Hughmilleria socialis sp. nov. Page 1091 1 Male operculate appendage. Natural size 3 Ventral view, showing metastoma and one gnathobase in position. Natural size 4 Swimming foot, disjointed, eine the form of the joints. x214 . Eurypterus pittsfordensis sp. nov. : Page 1098 2 Male operculate appendage. Operculum shows median cleft | and transversal suture. Natural size | | 5 Female second sternite, showing genital appendages. Nat- " ural size eee 6 Large sternite, showing paraeal suture. Natural size CRUSTACEA Rep. Paleontologist 1902. Plate 25 G.S. Barkentin, del. The Argus Co. State Printers. A.Hoen & Co. hth. Cee cael Sans rivers oS. n! Se oleate mane: Sa Nia tele be . » i - i ¥ PLATE 26 Unknown Eurypterid ol Page 1105 Ue nT 1 Imperfect arm. Natural size 2 Group of arms and one body segment. Natural ‘size 4 Imperfect arm. Natural size . Hughmilleria socialis sp. nov. : Page 1091 | 3 Female appendage of second sternite. Natural size | | 5 Coxal joint of fourth endognathite, showing large perfora of the upper side. x2 CRUSTACEA Rep. Paleontologisi 1902. Plate 26 pe ; The Argus Co. State Printers. A.Hoen & Co. hth. ( us ee eee Yiez : 4 ‘ “ - RiAsS : $ a is Ak of “iy or ; * : i A - r 5 mi rm hi 3 ft 1292, = ~——s* NEW YORK STATE MUSEUM ee PLATE 27 Protonympha ‘salicifolia nov. Page 1237 ; mens. All eal size and a from me sandstones with sonema, lying above the horizon of the Intumescens 20) tage. aaieetes Figures 1 and 2 are from ae au : Tanners gully, Wabi DEVONIC WORMS . Rep Paleontolosist 1902. Plate 27 G.S.Barkentin. del. W.S.Barkentin, lith. 1294 — NEW YORK STATE MUSEUM PLATE 28 Protonympha salicifolia nov. [See Pl. 27] Page 1237 1 Drawn from a plaster cast of the natural surface Palaeochaeta devonica nov. Page 1238 . 2 A small coiled ‘specimen. x2. From the soft shales in Grimes gully, Naples 3 “Rig 3 A larger but imperfect worm from the Tannery gully, Naples. x1.5 i, 4 A still larger specimen from the same loeality. x1.5 » DEVONIC WORMS e@) N 3) pus) 9) cc Ay ith. ] Barkentin S Ib de G.S.Barkentin INDEX Page numbers referring to descriptions of fossils*are printed in black face type. Accessions, 874-76. Acervularia (?) inequalis, 1117, 1125, 1126, 1128. ! Acidaspis ‘E-tuberculata, 1208. Acrotreta baileyi, 941. cf. belti, 938, 941. bisecta, 938,941. 3 Actinopteria arenaria, 1208. textilis, 1188, 1191, 1208. Agelacrinites, 994. Albany county, mastodons, 929-30. Allerisma?n.sp., 994, 995. ~ Ambocoelia, 905-6, 1203. sp. nov., 1203, 1207. umbonata, 905, 906, 1018.. mut. pluto, 905-6. explanation of plate, 1242. mut. pygmaea, 905. explanation of plate, 1242. var. gregaria, 905. Ami, cited, 951. Ampycidae, 946. Anastrophia verneuili, 1056, 1189, 1197, 1203, 1207. Angola shales, exposures, 1029. Annelida, 1081, 1234. Anoplia nucleata, 1191, 1203, 1207. Anoplotheea acutiplicata, 1207. concava, 1191, 1207. flabellites, 1207. Aphrodite, 1234. Arenicolites, 993. Asaphidae, 942, 946. Ashburner, C. A., cited, 979. 1491.) 1197. 1202, 1059, Aspidocrinus scutelliformis, 1191, 1193, | 1206. Ast, Philip, lithographer, 871; rial tribute to, 872-73. Athyris angelica, 990, 992, 993. cora, 992. __ polita, 995. memo- 1203, Atrypa lamellata, 1044, 1049. reticularis, 861, 1054, 1055, 1056, 1060, 1061, 1064, 1070, 1117, 1118, 1119, 1126, 1128, 1146, 1148, 1150, | 1151, 1L73, 1183; 1189, 119i 11935, | 1197, 1205, 1207. | spinosa, 1204, 1207. Atrypina imbricata, 1189, 1191, 1207. Aulopora, 1006, 1017. sp., 1203. sp.?, 1206. Aviculopecten?, 992, 995. sp.?, 992, 993, 995. eancellatus, 992. duplicatus?, 993. patulus, 994. rectirostra, 1203, 1208. | rugaestriatus, 992. spinulifer (?), 1057. tenuis, 993. Bactrites, 915-16, 1014. sp. mut. parvus, 916. explanation of plate, 1248. | sp. mut. pygmaeus, 915. explanation of plate, 1246. _ Barkentin, George 8., draftsman, 871. Barrande, cited, 1081, 1108. | Barrett, S. T., cited, 1149. ' Beachia suessana, 1202, 1203, 1208. | Becraft limestone, 1060-63, 1064 : | thickness, 1034; exposures near | Rondout, 1191-938, 1219, 1221, 1222, 1223, 1224, 1225; fauna, 1193. | Becraft mountain, stratigraphy, 862- | 63, 1030-79; topographic map of area, 863; geologic maps, 1032; | tectonic features, 1071-79. | Becraft region, strata, 1034. | Beecher, C. E., cited, 925, 932, 1045, | 1108; mentioned, 1033. | Bellerophon sp., 994, 1117. — | auriculatus, 1119, 1124, 1127, 1128. | maera, 993. 1296 Benham, W. Blaxland, cited, 1235. Bertie formation, 1167. Beushausen, cited, 1231. Beyrichia, 918. sp, L118) 11205-1121 St 2272S: 1IZES MAS M33 Iai SLs: sp.?, 1185. dagon, 918. explanation of plate, 1248. Bilobites varicus, 1189, 1206. Black shale, 1017. Bossardvillelimestone, 1153, 1166, 1175. Bothriolepis, 991. Sp. 90a. minor?, 994. Brachiopoda, 1006, 1008, 1009, 1017, 1026, 1027, 1028, 1029, 1081; dwarf fauna, 900-7. Brachyprion majus, 1203, 1206. schuchertanum, 1203, 1206. Bristol shales, exposures, 1013, 1018, 1029. : Brégger, cited, 938, 942, 943, 944, 945, 946, 951, 955. Bronteus barrandi, 1188, 1208. Bryograptus, 948, 954. sp., 949. kjerulfi, 944, 955, 956. lentus, 938. patens, 938. spinosus, 938. Bryozoan, 995, 1188. sp.?, 995, 1150. Bucania sp., 1117, 1127, 1133. Buchiola, 911. retrostriata mut. pygmaea, 911. explanation of plate, 1242. speciosa, 1017, 1021. ‘‘Bullhead’’ limestone of Erie county, 1138-41. Burden conglomerate, 1034-36. Butts, Charles, work of ,“869, 871, 967, 985; Conglomerate, 990-95. Calcareous concretions, 1008, 1020. Calcilutite, 1039. Callaway, cited, 945. Callograptus salteri? cj. Dendrograptus | sp., 954. Fossil Faunas of the Olean | ‘ ; | Cattaraugus county, mastodon, 933. | Cayuga Lake, NEW YORK STATE - Campbell, M. R., cited, 986. MUSEUM Calvmmene blumenbachii, 947. camerata, 1118, 1119, 1127, 1128, 1151. niagarensis, 1118, 1127, 1128, 1149, Tae Camarotoechia, 1202. allegania, 979, 991, 994. 995. barrandii, 1207. contracta, 992, 993, 994. var. robusta, 993. duplicata, 992. fitchiana, 1203, 1207. hudsonica, 1048-50. multistriata, 1203, 1207. neglecta, 1048, 1049, 1050, 1117, 1119). 1120, 1121, 1124 eo 1126, 1128, 1150; 1151, 1174. oblata, 1203, 1207. pliopleura, 1203, 1207. sappho?, 993, 994. sappho, 995. Cambric, importance of Dictyonema horizon for determination of upper boundary, 942, 956-58. | Cambric Dictyonema fauna in the slate belt of eastern New York, 934-58. Canandaigua quadrangle, areal and ~ paleontologic maps, 869-70: Carbonic formations of southeastern New York, 967-89. Carcinosoma newlini, 1108. ‘Carll, J. F., cited, 975, 976, 987, 988. Cashaqua shales, exposures, 1002-4, 1010, 1011, 1012, 1013, 1014, 1015, 1016, 1018, 1019, 1020, 1021, 1029; thickness, 1010. Catenipora labyrinthica, 1109. _Catskill sedimentation, not restricted to Devonic time, 998. Cattaraugus beds, 971-78; 997; fossils, 9938-94. age, 985, Cobleskill section at Union Springs, 1129-36. Cayugan, exposures near Rondout, 1183. hte Cephalopoda, 1020, 1023, 1026, 1027, 1081, 1156; dwarf species, 914-17. . INDEX TO REPORT OF THE STATE PALEONTOLOGIST 1902 Ceratiocaris (Limnocaris) praecedens, | 868, 1081. Ceratopyge, 946. Chaetetes sp., 1120, 1121, 1125, 1126, 1206. Spi, L197. (Monotrypella) arbusculus, 1132, 1134, 1137. sphaericus, 1188, 1189, 1190, 1191, 1203, 1206. Chaetopod worms, 1234. Champlainic, exposures near Rondout, 1180-81. Champlainic sandstone and Wilbur limestone, unconformity between, 1209-10. Chapman, cited, 960. Chautauqua county, m mastodons, 933. Chautauqua ages 867.7" Cheiruridae, 942, 946. © 2.44 Chemung beds, 968-71, 1011: age, 985 ; ’ fossils, 992-98, 1008,.1010. Chemung county, fossils collected in area covered by the Elmira quad- | rangle, 883-90. Chocolate shales, 990. Chonetes sp., 1191. sp.?, 1207. cf. arcuatus, 1070. hudsonicus, 1203, 1206. jerseyensis, 1117, 1118, 1126, 1128, 1133, 1134, 1161, 1166, 1173. lepida, 1020. scitulus, 992, 993. undulata, 1133, 1134. Chonophyllum, 1070. Chonostrophia complanata, 1203, 1206. Cirripede, 1204, 1208. Cladopora rectilineata, 1174. smicra, 1206. styphelia, 1066, 1067. | Clapp, F. G., work on Elmira quad-— rangle, 855, 871. Clark, P. Edwin, van Ingen, Gilbert &, Disturbed Fossiliferous Rocks in the | Vicinity of Rondout N. Y., 1176- | 1227; mentioned, 1063, 1064. | Clarke, John M., Mastodons of New | York, 921-33; Construction of the > Olean Rock Section, 996-99; inves- | 1297 tigations on fossils of Olean quad- rangle, 985; Torsion of the Lamelli- branch Shell, 1228-33; Some De- vonic Worms, 1234-38; cited, 862, 893, 932, 933, 1032, 1036, 1045, 1063, 1065, 1068, 1070, 1081, 1108, 1113, 1130, 1131, 1139, 1158, 1194, 1196, 1197,.1202, 1205,-1227. Claypole, cited, 1108. Climacograptus pungens, 1036. _ Climactichnites, 959-66. wilsoni, 960. Clinton group, 1111. Clinton limestone, 1116, 1167. Clonograptus, 948, 949, 952. (Dichograptus) flexilis, 947, 955, 956. milesi, 938, 939, 940, 947, 956. proximatus, 936, 938, 939-40, 947. tenellus, 940, 955. - Cobleskill limestone, age, 1113, 1131, 1145; age of the shales below, 1170-71; basal member, 1120; dip, 1135; exposures near Rondout, 1182-83, 1184; fauna and _ strati- graphic relations, 855-58, 1109; Guelph element in the fauna, 1156; fauna in Schoharie county, 1116-29, 1155; fossils at Frontenac island, 1132-34; field work, 858-62; rela- tion to overlying rock, 1121; Salina deposits, 1158-60; sections showing order of succession, 1111; first use of term, 1114; thickness, 862, 1120, 1140, 1143, 1144, 1169, 1170; of Erie county, 1138-41; in Herkimer county, 1169; section at Howes Cave, 1114-15; of the Hudson river valley, 1141-55; 5¢, cloth. Museum memoirs 1889-date. Q. 1 Beecher, C: E. & Clarke, J: M. Development of some Silurian Brachiopoda. 96p. Spl. Oct. 1889. Out of print. 2 Hall, James & Clarke, J: M. Paleozoic Reticulate Sponges. 350p. il. 70pl. 1898. $1, cloth, Aboriginal Occupation of New York. 190p.16pl. 2 maps Mar. MUSEUM PUBLICATIONS ~ 83 Clarke, J: M. The Oriskany Fauna of Becraft Mountain, Columbia Co: N. Y. 128p. 9pl. Oct. 1900. Soc. 4 Peck,C:H. N. Y. Edible Fungi, 1895-99. 106p. 25pl. Nov. 1900. 756. This includes revised descriptions and illustrations of fungi reported in the 49th, 5] st and 52d reports of the state hotanist. 5 Clarke, J: M. & Ruedemann, Rudolf. Guelph Formation and Fauna oe N ew York State. 196p. 21pl. July 1903. $7.50, cloth. Bie 6 Naples Fauna in Western New York. In press. Felt, E. P. Insects Affecting Park and Woodland Trees. In preparation. Merrill, F:J.H. Geology of New York City and Vicinity. Jn preparation. Ruedemann, Rudolf. Graptolitesof New York. Pt 1 Graptolites of the Lower Beds, In preparation. Natural history of New York. 30v.il. pl.maps. Q. Albany 1842-94. DIVISION 1 zooLoey. DeKay, JamesE. Zoology of New York; or, The New York Fauna; comprising detailed descriptions of all the animals hitherto ob- served within the State of New York with brief notices of those occasionally found near its borders, and accompanied by appropriate illustrations. 5v. il. pl. maps. sq.Q. Albany 1842-44. Out of print. Historical introduction to the series by Gov. W: H. Seward. 178p. v.1ptl Mammalia. 13-+146p. 33pl. 1842. 300 copies with hand-colored plates. v.2pt2 Birds. 12+380p.141pl. 1844. Colored plates. v.38 pt3 Reptiles and Amphibia. 7+98p. pt4 Fishes. 15+415p. 1842. pt3-4 bound together. ; v.4 Plates to accompany v.3. Reptiles and Amphibia 28pl. Fishes 79pl. 1842. 300 copies with hand-colored plates. : v.d pt} Mollusca. 4+27!p. 40pl. pt6 Crustacea. 70p. 18pl. 1843-44. Hand-colored plates : pt5-6 bound together. DIVISION 2 BOTANY. ‘Torrey, John. Flora of the State of New York ; ; comprising full descriptions of all the indigenous and naturalized plants hitherto discovered in the State, with remarks on their economical and medical properties. 2v. il. pl. sq. Q. Albany 1843. Out of print. v. 1 Flora of the State of New York. 12+484p. 72pl. 1843. 800 copies with hand-colored plates. v. 2 Flora of the State of New York. 572p. 89pl. 1843. 300 copies with hand-colored plates. DIVISION 3 MINERALOGY. Beck, Lewis C. Mineralogy of New York ; : comprising: detailed descriptions of the minerals hitherto found in the State of New York, and notices of their uses in the arts and agriculture. il. pl. sq. Q. Albany 1842. Out of print. v. 1 ptl Economical Mineralogy. pt2 Descriptive Mineralogy. © 24+-536p. 1842. 8 plates additional to those printed as part of the text. ; DIVISION 4 GEOLOGY. Mather, W: W.; Emmons, Ebenezer ; Vanuxem, Lardner & Hall, James. Geology of New York. 4yv. il. pl. sq. Q. Albany 1842-43. Out of print. vgs v.1 ptl Mather, W: W. First Geological District. 387-+6538p. 46pl. 1843. v.2 pt2 Emmons, Ebenezer. Second Geological District. 10-+487p. 17pl. 1842. v.3 pt3 Vanuxem, Lardner. Third Geological District. 306p. 1842. v.4pt4 Hall, James. Fourth Geological District. 22+683p. 19pl. map. 1843. DIVISION 5 AGRICULTURE. Emmons, Ebenezer. Agriculture of New York; ‘com prising an account of the classification, composition and distribution of the soils and rocks and the natural waters of the different geological formations, together with a condensed view of the meteorology and agriculturai produc-. tions of the State. 5v. il. pl. sq. Q. Albany 1845-54. Out of print. v. 1 Soils of the State, their Composition and Distribution. 11-+-371p. 21pl. 1846. 5 UNIVERSITY OF THE STATE OF NEW YORK vy.2 Analysis of Soils, Plants, Cereals, etc. 8+3848+46p, 42pl. 1849. With hand-colored plates. v.3 Fruits, etc. 8+4340p. 1851. vy.4 Plates to accompany v. 3. 95pl. 1851. Hand-colored. y.5 Insects Injurious to Agriculture. 8+272p. 50pl. 1854. With hand-colored plates. DIVISION 6 PALEONTOLOGY. Hall, James. Palaeontology of New York. 8v. il. pl. sq.Q. Albany 1847-94. Bound in cloth. y.1 Organic Remains of the Lower Division of the New York System. 23-+-338p. 99pl. 1847. Out of print. y.2 Organic Remains of Lower Middle Division of the New York System. 8+362p. 104pl. 1852. Out of print. y.3 Organic Remains of the Lower Helderberg Group and the Oriskany Sand- stone. ptl, text. 12+5382p. 1859. [$3.50] : ——pt2, 143pl. 1861. [$2.50] v.4 Fossil Brachiopoda of the Upper Helderberg, Hamilton, Portage and Che- mung Groups. 11+1-+428p. 99pl. 1867. $2.50. vy.5 pti Lamellibranchiata 1. Monomyaria of the Upper Helderberg, Hamilton and Chemung Groups. 18+268p. 45pl. 1884. $2.50. Lamellibranchiata 2. Dimyaria of the Upper Helderberg, Hamilton, Portage and Chemung Groups. 62-+298p. 5Ipl. 1885. $2.50. —pt2 Gasteropoda, Pteropoda and Cephalopoda of the Upper Helderberg, Hamilton, Portage and Chemung Groups. 2v. 1879. v.1, text. 15+492p. v. 2,120p]l. $2.50 for 2 v. y.6 Corals and Bryozoa of the Lower and Upper Helderberg and Hamilton Groups. 24+298p. 67pl. 1887. $2.50 v. 7 Trilobites and other Crustacea of the Oriskany, Upper Helderberg, Hamil- ton, Portage, Chemung and Catskill Groups. 644-236p. 46pl 1888. Cont. - supplement to v. 5, pt2. Pteropoda, Cephalopoda and Annelida, 42p. 18pl. 1888. $2.50. . ; vy. 8 pti Introduction to the Study of the Genera of the Paleozoic Brachiopoda. 16+367p. 44pl. 1892. $2.50. —— pt2 Paleozoic Brachiopoda. 16+394p. 84pl. 1894. $2.50. Handbooks 1893-date. 7$x124 cm, In quantities, 1 cent for each 16 pages orless. Single copies postpaid as below. H5 New York State Museum. 52p.il. ge. Outlines history and work of the museum with list of staff 1902. H13 Paleontology. 12p. 2c. _ Brief outline of State Museum work in paleontology under heads: Definition; Relation to biology; Relation to stratigraphy; History of paleontology in New York. H15 Guide to Excursions in the Fossiliferous Rocks of New York. 124p. Se. Itineraries of 32 trips covering nearly the entire series of Paleozoic rocks, prepared specially for the use of teachers and students desiring to acquaint themselves more intimately with the - elassie rocks of this State. a; H16 Entomology. 16p. 2c. H17 Economic Geology. In preparation. H18 Insecticides and Fungicides. 20p. je. H19 Classification of New York Series of Geologic Formations. 32p. 3c. Maps. Merrill, F: J. H. Economic and Geologic Map of the State of New York; issued as part of Museum bulletin 15 and the 48th Museum Report, v. 1. 59x67 cm. 1894. Scale 14 miles to 1 inch. Separate edition out of eront. Geologic Map of New York. 1901. Scale 5 miles to 1 inch. Jn atlas jorm $3; mounted on rollers $5. Lower Hudson sheet 6oc. The lower Hudson sheet, geologically colored, comprises Rockland, Orange, Dutchess, Put- nam, Westchester, New York, Richmond, Kings, Queens and Nassau counties, and parts of aes Ulster and Suffolk counties; also northeastern New Jersey and part of western Con- necticut. Map of New York showing the Surface Configuration and Water Sheds. 1901. Scale 12 miles to 1 inch, 156. ——- 3 “ sentisarennate | JOHN M CLARKE STATE PALEONTOLOGIST HUDSON RIVER GROUP Quarry © Horizontal #Syneline + Anticline @> Pitch of axis of fold” + Vertical Ais Strike and dip 7 UNIVERSITY OF THE STATE OF NEW YORK STATE MUSEUM ANNUAL REPORT 1902 Y Ch Claver STRATIGRAPHIC AND PALEONTOLOGIC MAP 0 Bo BECRAFT MOUNTAIN COLUMBIA COUNTY NEW YORK BY AMADEUS W.GRABAT 1903 Based on a topographic map executed under the direction of C.C. VERMEULE for Dr. JOHN C.SMOCK ‘ 1900 Seale, 6 inches - 1 mile © 200 400 v0 800 1000 ; ulejunou yeis9g jo deur s130jo3u0a{ed pue s1ydeisijeIys n Oo pe) te oO =] (7) ° ps. w o QO “t ~ oe) 3 ° c 3 ct ) pete = \ & $ FE ‘ > i : ‘ ' 0s ) x " 4 { BE nk Mak mi Ses ae agi P > - aan sco ( | panes caer ee gue” ett aah eee el Aa Re Par ee wens gare 9 an carte «nly % HUDSON RIVER GROUP LEGEND aa Esopus oe. Oriskany } Port Ewen (ied E : i 42 Quarry + Vertical ¥ Syncline ® Horizontal Ais Strike and dip + Anticline @ Pitch of axis of fold Po ee UNIVERSITY OF THE STATE OF NEW YORK STATE PALEONTOLOGIST STATE MUSEUM ANNUAL REPORT 1902 eer SOLOSS Se Ds MAN, The Argus Co State Printers GEOLOGY AND PALEONTOLOGY oF BECRAFT MOUNTAIN SECTIONS 7 TO 20 SOALE 1 IN. 250 FT. SuRvermp axp Dawn sy A. W. GRABAU, 1902-03 eS - 25 egoeeet ie: 5 ee TRAE R et; eee Pa Toa Tn sn