CORNELL UNIVERSITY LIBRARY GIFT OF iiev York State Library Cornell university Library QE 779.R91 '■* GraptoMesofNewYofkj Cornell University Library The original of this book is in the Cornell University Library. There are no known copyright restrictions in the United States on the use of the text. http://www.archive.org/details/cu31924004415380 New York State Education Department New York State Museum John M. Clarke, Director Memoir ii GRAPTOLITES OF NEW YORK Part 2 GRAPTOLITES OF THE HIGHER BEDS BY RUDOLPH EUEDEMANN Preface ------ 4 Introduction ----- 9 Range and geographic distribution 9 Correlation table of zones - Faces 10 Synoptic view of range of genera ii(i Synoptic table of range of genera Faces (>(> Additional notes on morphology - 69 Notes on phylogeny - - - - 107 Synoptic list of graptolites noted in this volume - - 127 Synoptic and synonymic list of grap- tolites of North America - 130 Additional references - - - 140 Descriptions of graptolites - - 145 Dendroidea . - - . - 145 Graptoloidea .... 247 Axonolipa - - - - - 247 Axonophora - . - . 339 Addendum 484 Explanation of plates - - . 489 Index 559 ALBANY NEW YORK STATE EDUCATION DEPARTMENT 1908 STATE OF NEW YORK EDUCATION DEPARTMENT Regents of the University With years when terms expire 191 3 Whitelaw Reid M.A. LL.D. D.C.L. Chancellor - New York 191 7 St Clair McKelway M.A. LL.D. Vue Chancellor - Brooklyn 1908 Daniel Beach Ph.D. LL.D. Watkins 1914 Pliny T. Sexton LL.B. LL.D. .... Palmyra 1922 T. Guilford Smith M.A. C.E. LL.D. .... Buffalo 1918 William Nottingham M.A. Ph.D. LL.D, - - Syracuse 1910 Charles A. Gardiner Ph.D. L.H.D. LL.D. D.C.L. - New York 191 5 Albert Vander Veer M.D. M.A. Ph.D. LL.D. - Albany 1911 Edward Lauterbach M.A. LL.D. .... New York 1909 Eugene A, Philbin LL.B. LL.D. .... New York 1916 LuciAN L. Shedden LL.B. ... - . Plattsburg Commissioner of Education Andrew S. Draper LL.B. LL.D. Assistant Commissioners Howard J. Rogers M.A. LL.D. Fzrsl Assistant Edward J. Goodwin Lit. D. L.H.D. Second Assistant Augustus S. Downing M.A. Pd.D. LL.D. Third Assistant , Director of State Library Edwin H. Anderson M.A. Director of Science and State museum John M. Clarke Ph.D. LL.D. Chiefs of Divisions Administration, Harlan H. Horner B.A. Attendance, James D. Sullivan Educational Extension, William R. Eastman M.A. M.L.S. Examinations, Charles F. Wheelock B.S. LL.D. Inspections, Frank H. Wood M.A. Law, Thomas E. Finegan M.A. School Libraries, Charles E. Fitch L.H.D. Statistics, Hiram C. Case Visual Instruction, DeLancey M. Ellis New York State Education Department Scie7ice Division, J2ine 26, igo^ Hon. A, S, Draper LL.D. Covimissioncr of Education Dear sir : I communicate herewith for publication as a memoir of the State Museum, the manuscript and accompanying plates of part 2, Graptolites of New York prepared by Dr R. Ruedemann, Assistant State Paleontologist. Part I of this work was published in 1905 and has met a most appreci- ative reception amongst the paleontologists of the world. The present contribution concludes the investigations which have been under way for a period of several years. Very respectfully John M. Clarke Director State of New York Education Department commissioner's room I Approved for publication this 28th day of Ju7te igoj Commissioner of Education PREFACE The first instalment of the graptoUtes of New York was pubHshed as Memoir 7, New York State Museum. It comprises a resumd of the present status of our knowledge of graptolites and descriptions of the graptolites of the Upper Cambric and Lower Champlainic (Lower Ordovicic). The present volume contains the remainder of the graptolites, i. e. those of the Middle and Upper Champlainic, the Siluric and Devonic. The correlation of the New York graptolite beds with those of other parts of America made it necessary to institute comparisons with graptolites from other states and the occasion has been used to describe and figure the relatively small number of forms from other parts of the country as far as these have been made accessible to us through the kindness of colleagues. The rich faunas of Canada have been excluded since we are informed that Professor Lapworth, the leader among modern investigators in this field, has been studying them for more than a decade. During the prosecution of this investigation, the desirability of some introductory chapters to the second part of the treatise has urged itself upon the writer. These are wholly supplementary to those of the first part and contain bibliographic references, and morphologic and phylogenetic observations regarding the later graptolites here described. Some obser- vations have been incorporated in the introduction because they could be dealt with more advantageously here than when scattered through generic and specific descriptions. The discussion of the range of the forms and the geographic distribution of the zones of the higher graptolite beds had for obvious reasons also to be reserved for this volume. A more complete cor-. relation table of the zones incorporating those of the first volume is added ; and also a synoptic table of the range of the genera of the higher beds. Finally, we have in completion of our work inserted a synoptic and syn- onymic list of the graptolites known from North America. A few notes on forms which at times have been considered as graptolites have been added in an appendix. GRAPTOLITES OF NEW YORK, PART 2 5 During this investigation of the higher graptolite faunas it has been found necessary to ask from the Director of the United States Geological Survey the loan of the types of a number of new species, mostly from the Normansklll shales of New York (Stockport, Columbia co., N. Y.), which had been described, but not figured, by Dr R. R. Gurley In the Journal of Geology [v. 4, 1896]. Our request was most liberally granted by the authorities of the United States Geological Survey and of the National Museum, but with the specimens there was delivered to us the voluminous unfinished manuscript of Gurley's monograph of the graptolites with the understanding that we should use as much as possible of the same, and thus assure to Dr Gurley's long labors, the credit to which they are entitled. The author has gladly availed himself of Gurley's work, which even In its fragmentary form bears witness not only of the admirable patience and enthusiasm of Its author, but also of his keen power of observation. In justice to both Dr Gurley and myself a full statement of what this voluminous manuscript contains and what has been used for this memoir, should be given in this place. The greater part of the manuscript consists of copies of the descrip- tions, and translations of those In other than the English language, of all foreign species of graptolites together with a full bibliography of all species described up to 1896. It is obvious that it was the author's intention to produce a monograph of all the graptolites of the world. Another part of the manuscript contains the history and synonymy of the American species. In this work Dr Gurley had evidently made special efforts to trace the history of many of the cryptic names of the earlier geolo- gists, as those of the graptolites mentioned In the reports of the first geo- logical survey of New York by Emmons and others. These notes are fairly complete ; they have been used here as far as the scope of our work allowed and due credit given the author. In the description of the North American graptolites Gurley had not proceeded beyond the Dendroldea and a part of the Graptololdea of the Lower Champlainic. The former consist In the large majority of the 6 NEW YORK STATE MUSEUM Niagaran forms from Hamilton, Canada, which lie without our field, and the descriptions of the latter faunas are entirely based upon Canadian material. Moreover, the Graptoloidea of the Lower Champlainic have already been described in Memoir 7 as far as they are found within the boundaries of the State. Of this part of the manuscript there could, for these reasons, be used only the descriptions of a few new Dendroidea from the Niagaran and the Devonic of New York. In case Professor Lapworth should not have extended his work to the remarkable Dendroid fauna of Hamilton, first made known by Spencer, this part of Gurley's work could easily be made complete by the addition of the descriptions of the few western forms and would become a valuable contribution to paleontology. The drawings of a considerable portion of the Dendroidea are finished ; they are pen drawings made on blue prints from photographs, and very cor- rect and effective. A few of them representing the New York species have been used in this publication, supplemented by camera enlargements. The manuscript is accompanied by a considerable number of pen draw- ings of graptolites other than Dendroidea. These, being free-hand drawings made by a draftsman, are mostly diagrammatic though carefully executed. We have inserted them in the case of Gurley's new species in the text as his original drawings and supplemented them by camera enlargements and tracings from the types as far as the latter could be found. J\. very valuable addition to the material sent from Washington is a manuscript report by Professor Lapworth on a collection of Stockport, N. Y. graptolites sent to him by Dr Gurley. It contains the descriptions of the new Normanskill species published in 1896 in Xh& Journal of Geology, We have taken the liberty of incorporating Lapworth's important notes on Diplograptus foliaceus in our paper. On the whole, it may be fairly said that Dr Gurley has printed in his preliminary publication in the Journal of Geology all that was new or especially worthy of publication, namely the descriptions of all new species — with the exception of a few Dendroidea — and his observations on the morphology of certain hitherto incompletely known species (e. g. C 1 a t h- GRAPTOLITES OF NEW YORK, PART 2 7 rograptus geinitzianus). Still, there was enough left in the manu- script to make it a welcome help to the writer in many ways. Its extensive bibliography of the graptolites, which is practically complete to 1896, might be published as a separate bulletin, as also eventually the Dendroidea. This done, full justice, I believe, would have been rendered to Dr Gurley's assiduous labors on the graptolites. For the loan of collections and for valuable information I am sincerely thankful to Director Charles D. Walcott, Dr T. W. Stanton, Dr E. O. Ulrich, Mr Ray S. Bassler of Washington, to Prof. T. W. Sardeson of Minneapolis, Prof. Charles Schuchert of New Haven, Mr John Schuler of Rochester, Mr Edwin Kirk and Prof. R. P. Whitfield of New York. April /, igoj Rudolf Ruedemann Assistant State Paleontologist GRAPTOLITES OF THE HIGHER BEDS RANGE AND GEOGRAPHIC DISTRIBUTION In part i of the Graptolites of New York we have drawn the division line between the Lower and Upper Graptolite faunas of New York above the third Deepkill zone (zone with Diplograptus dentatus). The reasons for this proceeding were partly of a practical and partly of a theoretical nature ; on one hand we thus obtained an approximately equal division into halves of the subject-matter, and on the other since that zone had been roughly correlated with the Chazy formation, we left all the zones of the Canadian or Paleochamplainic period (the first of the three periods of the Champlainic) in association as they are usually found in the field. But we have already emphasized the fact that while the genera of the Axonolipa, which are characteristic of the Lower Graptolite fauna, viz, Dichograptus, Loganograptus, Tetragraptus and Phyllograptus, become extinct with this third zone, the Axonophora, which are characteristic of the Upper Graptolite fauna, appear abruptly in it with their important genera Diplograptus, Glos- sograptus and Climacograptus. The third Deepkill zone is hence truly transitional between the Lower and Upper Graptolite faunas, and if the now prevailing principle, that the division lines should be determined rather by the arrival of new forms than by the extinction of old ones, had been followed, this zone would have been joined to the Upper Graptolite fauna. It partakes, however, in this regard fully of the nature of its correlative, the Chazy formation, which also is more characterized by the advent of genera typical of the later Mohawkian, specially of the Trenton limestone, than by the extinction in it of the older genera of the Canadian era ; and as long as the latter is united into one period with the preceding Beekmantown lime- stone by the New York geologists we are justified in conforming in regard to the corresponding graptolite zone. Gurley [1896, p.304] has provisionally correlated certain small faunas from Mystic (Canada), Kicking Horse Pass (Canadian Rocky mountains) -and Dease river (British Columbia) with the Chazy limestone, but since lO NEW YORK STATE MUSEUM these, as far as known, contain only species of the Normanskill fauna (Lower Dicellograptus zone) which is now known by direct stratigraphic evidence [^see p. 1 1] to be of Trenton age, they would, as prenuncial faunas of the Trenton, seem to be more properly correlated with the Lowville and Black River limestones. Probably also the occurrence of Diplograptus foliaceus and Climacograptus scharenbergi in black limestone pebbles of the Rysedorph hill conglomerate [Ruedemann, 1901, p. 92] in association with a rich brachiopod and trilobite fauna, including Bronteus lunatus, Calymmene senaria, Ceraurus pleurexanthemus and Sphaerocoryphe major, is indicative of a horizon intercalated between the third Deepkill zone and the Normanskill zone ; for, although the writer in the paper before cited correlated this fauna of the black pebbles tentatively with the lower Trenton, a remoter (probably Black River) age has been claimed for it by some, apparently on good ground. I Normanskill shale (Zone of Nemagraptus gracilis or Dicellograptus zone) The first zone of the Upper Graptolite fauna fully developed in this State is that of the Normanskill shale. The most important forms of its rich fauna were originally discovered in a cliff on the bank of the Normans- kill, a small tributary of the Hudson emptying below Albany, and already described and beautifully illustrated in the first volume of the Palaeontology of New York. Further species, which were obtained when a railroad was built along this cliff, were described in a supplement to volume 3 of the same publication. The fauna was regarded by Hall as characterizing the "Hudson River shales" above the horizon of the Utica shale, a position which it held almost undisputed until 20 years ago when Lapworth, who had studied the same fauna from the Lower Canadian rocks, identified the zone with the British one of Coenograptus gracilis and since the latter corresponds to a part of the Llandeilo, inferred a younger (approxi- mately Black River-Trenton) age for the Normanskill zone.' The writer 'A full account of the history of this zone has been given by the writer in N. Y. State Mus. Bui. 42. GRAPTOLITES OF NEW YORK, PART 2 II showed in 1901 that the belt of slate which contains this fauna in the Hud- son river region underlies the Utica shale and correlated the zone with the lower or middle Trenton. Since then still more direct evidence for the Trenton age of the Nor- manskill Graptolite fauna has come to light. Weller [1903, p. 5 2] has found the fauna in New Jersey near the base of the shale formation, from 50 to 75 feet above the Parastrophia hemiplicata zone which is near the base of the Trenton limestone ; and, since the sequence from the Trenton lime- stone to the "Hudson River slates" at the locality is normal for New Jersey, concluded that the graptolite beds "would seem to be equivalent to about the middle portion of the typical Trenton limestone of New York, or even to a position below the m.iddle." Through the liberality of Prof. Eugene A. Smith, State Geologist of Alabama, the writer has had the privilege of studying a well preserved, slightly modified Normanskill fauna occurring in calcareous shale in Bibb county, Alabama, which is associated with Trenton limestone and according to Professor Smith of upper Trenton age. The following section of this interesting locality has been kindly furnished. Section at Pratt's Ferry, Bibb county, Alabama, in descending order : 1 Black shales, weathering yellowish and forming light yellow soil. Thickness not given feet 2 BlufE of bedded chert lo-i 5 Talus or slope of 40 feet vertical hight 3 Heavy bedded chert 1 5~2o 4 Sandstone iS 5 Beds of chert with Subcarboniferous fossils 20 6 Sandstones alternating with black slates, but mostly sandstone 60 7 Strata not seen 20 8 Calcareous shales with graptolites, bluish black but weathering gray or white breaking up into small shaly blocks 40 9 Thin bed of chert. Thickness not given 10 Gray calcareous shales like no. 8, graptolitic 100 11 A thin bed of sparry limestone full of small fossils and also graptolites (?), Thickness not given 12 NEW YORK STATE MUSEUM FEET 12 Calcareous shales full of graptolites 50 13 Sandy reddish shales breaking up into square-faced pieces 10 Below these fossiliferous limestones there are 600 to 800 feet of massive lime- stones and marble with Orthoceras. These include the Chazy (with Ma: dure a magna) and Trenton. The graptoHte beds are, as the section shows, at the top of the series, not far below chert beds with Subcarboniferous fossils. The fauna consists of the following species : Nemagraptus gracilis waf. surcularis /Ja/Z (r) Diplograptus foliaceus var. alabamensis Dicellograptus smithi nov. (cc) nov. (cc) D. moffatensis Carruthers var. alabamensis Climacograptus cf. putillus {Hall) (c) nov. (cc) Cryptograptus tricornis (Carruthers) (c) D. cf. mensurans nov. (rr) Glossograptus ciliatus Emmons (c) While the essential identity of this fauna with our Normanskill grapto- Hte fauna can not be gainsaid, this identity can not be taken as demonstrat- ing more than the general fact of the Trenton age of the Normanskill fauna, because, on one hand, the Alabama fauna contains enough differing elements to be not exactly identical and on the other hand it is open to question whether this upper Trenton of Alabama is exactly equivalent to ours. Hence while the Trenton age of the Normanskill zone can be consid- ered as well established, its exact place in the Trenton formation is still open to question. On the other hand, the position of the Normanskill fauna in New Jersey and Alabama excludes also the possibility that that fauna can be of greater than Trenton age ; hence it can not be placed between the Chazy and Trenton limestone as Lapworth provisionally assigned it. The fact that still another well differentiated zone [see postea p. 29] intervenes between those of the Normanskill and Utica shales and the marked difference of the Normanskill and Utica faunas argue strongly however for the position of the Normanskill shale below the upper Trenton. Since the original discovery of the zone at the Normanskill, numerous other localities, to be noted further on, have become known in the slate belt of eastern New York on both sides of the Hudson river. Walcott, In his investigation of the slate belt [1888] discovered many localities, espe- GRAPTOLITES OF NEW YORK, PART 2 13 cially in Washington and Rensselaer counties, and Dale and Prindle in their continuation of these studies have added considerably to the list of localities. During the construction of the West Shore Railroad Hall secured for the State Museum a very large collection of splendidly preserved graptolites — in fact the best preserved Normanskill graptolites known to the writer — from a cut near Glenmont station in Albany county, and the writer has obtained large collections from Mount Moreno near Hudson, Columbia county, and other localities, while Gurley has based his investigation of the fauna on a large collection secured by him at Stockport, also in Columbia county, N. Y. All these occurrences have demonstrated that the Normans- kill fauna is probably not only present in a large area of the slate belt of New York, but is also by far the most commonly met with of the graptolite faunas of the shales and slates of eastern New York, while it is absent out- side of the area of the former x\ppalachian basin, or from the central and northwestern part of the State where the shale is replaced by the Trenton limestone. The complete fauna, as known in this State, is given in the following table which shows its distribution in the four principal localities. TABLE 1 GRAPTOLITES OF THE NORMANSKILL SHALE IN NEW YORK Ptilograptus poctai nov Dictyonema spiniferum nov Odontocaulis hepaticus nov Desmograptus tenuiramosus nov Thamnograptus capillaris {E7nmons) Cf. Protovirgularia dichotoma McCoy Didymograptus sagitticaulis {Hall) Gurley 8 D. serratulus {Hall) 9 D. subtenuis {Hall) 10 Azygograptus walcotti Lapworth 1 1 A. ? simplex nov I 2 3 4 5 6 7 w o O w o o w o O w U O H OTHER LOCALITIES IN NEW YORK none none none none none Moordener kill Lansingburg Lansingburg 14 NEW YORK STATE MUSEUM TABLE 1 QRAPTOLITES OF THE NORMANSKILL SHALE IN NEW YORK {continued') 12 Leptograptus flaccidus timt. trentonensis nov... 13 id. var. spinifer viut. trentonensis nov 14 id. var. spinifer mut. trifidus nov 15 Syndyograptus pecten nov 16 Amphigraptus divergens {Hall ) 17 A. multifasciatus {Hall) 1 8 Nemagraptus gracilis {If all) 19 id. var. surcularis Hall 20 id. var. crassicaulis Gurley 2 1 id. var. distans nov 22 id. var. approxiraatus nov 23 N. exilis Lapworth 24 id. var. linearis nov 25 Dicellograptus mensurans nov • 26 D. divaricatus {Hall ) 27 id. var. rectus nov 28 id. var. bicurvatus nov 29 id. var. salopiensis Elks &" Wood 30 D. intortus Lapworth 3 1 D. gurleyi Lapworth 32 D. sextans {Hall) 33 id. var. exilis Elks is' Wood 34 id. var. perexilis nov 35 id. var. tortus nov 36 Dicranograptus nicholsoni var. parvangulus Gurky 37 id. var. diapason Gurley 38 D. ramosus Hall 39 D. spinifer Elks (s' Wood 40 id. var. geniculatus nov 41 D. furcatus Hall 42 id. var. exilis nov 43 D. contortus nov 44 Corynoides calicularis Nicholson . . 45 C. gracilis mut. perungulatus nov. , 46 Diplograptus foliaceus Murchison. 47 id. var. incisus Lapworth 48 id. var. acutus Lapworth 49 D. angustifolius Hall 50 D. euglyphus Lapworth 5 1 id. var. pygmaeus nov. 52 Glossograptus qX\2Xm% Emmons. .. . X X X X x x o A O El o U o OTHER LOCALITIES IN NEW YORK none none none none none none many Granville none none none Granville Speigletown none Granville Speigletown none none Speigletown Granville many none Granville many none Granville.Green- wicli,Wash. co. none none Speigletown many many many Speigletown Lansingburg GRAPTOLITES OF NEW YORK, PART 2 TABLE 1 QRAPTOLITES OF THE NORMANSKILL SHALE IN NEW YORK (concluded) 15 A •A H w U H OTHER LOCALITIES IN NEW YORK 53 id. var. debilis nov X X X X X 54 G. whitfieldi {Hall) X X X X X X X 55 Cryptograptus tricornis (Carruthers) many many Lansingburg Lansingburg 56 Climacograptus parvus Ifall X X X X X X KQ C scharenberefi Lai)worth X X 60 C bicornis Hall X X X X many Chatham 61 Re tio err ant us ffeinitzianus {Hall\ 62 Lasiograptus mucronatus {Hall) X X X Schodack land'g Moordener kill This wonderfully rich fauna, consisting of some 60 species of grapto- lites, is, however, in the great majority of the outcrops only preserved in a very fragmentary condition, i. e. in but a few of the most common and characteristic forms. Only the four localities given in the foregoing list, viz, Normanskill (Kenwood), Glenmont near Albany, Mt Moreno near Hudson, and Stockport in Columbia county have furnished complete or nearly complete faunas. Of these, Glenmont has yielded the most com- plete series, 41 forms, Mt Moreno 32, Stockport 30 and Normanskill 29. The faunas of all these four localities can be considered as typically repre- senting the Normanskill association and as being strictly of one horizon. The slight differences in their associations are probably largely referable to the greater or less completeness of the collections. A few notable differ- ences, not so readily explained, are the occurrence of the Dendroidea in the Glenmont collection alone (with the exception of Thamnograptus c a p i 1 1 a r i s ) and the scarcity of the Didymograpti in the same collection, while the latter prevail in the shales of Mt Moreno. i6 NEW YORK STATE MUSEUM The following is a list of smaller faunules (or collections) of this horizon, obtained in this State : TABLE 2 6 o < n o o < A •A u < p o a o H w ■ 1-1 H < It 2 « O o X > o H m CM >- o o X >< o H hT 5 2: w H en w o fM 6 u w in 2; w « H 2 < -1 6 o A w O ^< o M o z; d o O o si y5 z 1 o Oi u " z w o iJ H P o Q Z a w ° ^ ■^> N X X X X X X d J z J o '1 O tn . < Z ^ o Z a M X X d u , Z z o < H »i o o z fe £ O c/J < Sri . > H en Thamtiograptus capillaris (^Em- Mons\ X X X X X X X X X X X Didyniograptus sagitticaulis Guyley D. subtenuis (Hall) D serratulus (Hall\ Nemagraptus gracilis {Hall). . . id vaf surcLiIari*; ( FTall^ X id. var. crassicaulis Gurley X AzveroeraDtus ? simnlex nov . . . X X X X X X Dicellograptus sextans {Hall). . O divarioatiit; i WaJl\ X X X Dicranograptus ramosus Hall. . D. nicholsoni var. parvangulus Criirlev .. _.- X X X X X X id i)cty fi^a^>?l'^^n Crit.yJpv X X X X X D contortus nov X X X X X D furcatus Hall X X Corynoides calicularis Nicholson Diplograptus id\\z.c&M% Murchi- son X X .... X X X .... X X O ane^ustifoli lis TTnJI X X X X (x) X X X X X X — Cryptograptus tricornis {Carr). Climacograptus bicornis Hall . . X X X X X X X X X X X X X X Lasiograptus mucronatus {Hall) GRAPTOLITES OF NEW YORK, PART 2 1 7 As this list shows, none of the species appears in every collection, but a few species are mostly present. These are Nemagraptus gracilis, Dicellograptus sextans, D. furcatus, Diplograptus foliaceus, D. angustifolius, Climacograptus parvus and C . b i c o r n i s . It is further to be noted that, while the association in general may be said to have been everywhere the same in these localities, still one form is frequently found profusely and as the most common of all in one locality, while in the others it is absent. Thus Dicranograptus furcatus is extremely common at the locality i mile north of Granville and near McDougal's lake, Climacograptus parvus at Pittston corners and Dicranograptus ramosus 2^ miles north of Middle Granville. To know whether these dominant species will ever become the means of a further subdivision of the zone lies at present beyond the scope of our facts, though in view of the considerable thickness of the rocks carrying the Normanskill fauna a future subdivision seems quite possible and is certainly much to be desired. Nemagraptus gracilis has been considered the most character- istic form of the equivalent zone in Europe, and Lapworth has also termed this zone in Canada the "zone with Coenograptus gracilis." It is, however, possible, according to Ami's observation, that this species passes also into the next zone. Dicellograptus sextans, Dicrano- graptus furcatus and Climacograptus parvus are, of the more abundant forms, apparently most strictly bound to this zone and therefore among its best index fossils. The genera, which pass but little below and above this horizon, and here distinctly reach their climax by the number of different forms, size and number of individuals, are Nemagraptus, Dicellograptus and Dicranograp- tus. The term Lower Dicellograptus subzone, proposed by Gurley [1892, p,403] is therefore quite appropriate with the limitation, that, since the next zone is markedly free from Dicellograpti the term Upper Dicello- graptus zone is better replaced by another and the lower zone may be 1 8 NEW YORK STATE MUSEUM simply termed the Dicellograptus zone. Altogether, the fact of the great difference in the faunal expressions of this and the following zone, in which the biserial forms entirely dominate and the distinct presence of faunules, which eventually may be recognized as subzones of the Dicellograptus zone, necessitate the recognition of the latter as a separate unit. One of these subzones is quite obviously represented by a faunule collected by the writer at the power house of the traction company, north of Lansingburg. While having in common with the other outcrops of Normanskill shale the species: Didymograptus serratulus, Azygograptus ? simplex, Dicranograptus ramosus, Climacograptus parvus, C. modestus, C. bicornis and Diplograptus foliaceus, this faunule contains in Diplograptus amplexicaulis var. pertenuis, Diplograptus euglyphus van pygmaeus, Climacograptus putillus mut. e x i m i u s and Corynoides gracilis, peculiar elements of its own. It is characterized by the great prevalence of minute Diplograpti and Climaco- grapti (C. modestus, C. parvus, C. putillus mut. e x i m i u s ) and would seem to represent for this reason a transition to the next zone. Another peculiar association has been observed by me near Speigle- town, north of Troy. It consists of Nemagraptus exilis var. linearis Corynoides gracilis mut. perungulatus Dicellograptus divaricatus var. rectus Diplograptus euglyphus D. intortus The localities mentioned in the foregoing tables are situated in the two belts of Champlainic rocks which with some interruptions flank the Lower Cambric slates of the slate belt of eastern New York. They lie in Colum- bia, Rensselaer and Washington counties or on the east side of the Hudson river, with the exception of those of No/manskill (Kenwood) and Glenmont, which are in Albany county and on the west side of the river. The zone itself has not yet been mapped, with the exception of a small area in the neighborhood of Albany in a former paper of the writer [1901] and its car- tographic fixation will, no doubt, lead to a distinction of its subzones and of GRAPTOLITES OF NEW YORK, PART 2 1 9 their relative positions. In the broad belt of " Hudson River shales " extending south and southeast of Columbia county, into New Jersey, few localities have become known. One of these, consisting of the cuts of the West Shore Railroad near Highland, opposite Poughkeepsie, was made known by Booth in 1883. Among the graptolites identified by Whitfield from this outcrop are Nemagraptus gracilis, Didymograptus sagitticaulis, Dicranograptus furcatus and Cryptograp- tustricornis. The museum of Columbia University also contains a small series of graptolites from Poughkeepsie indicating the presence of this horizon in Dutchess county. \r\. New Jersey, graptolites referable to the Dicellograptus zone have been found in two localities [Weller, 1903, p. 5 2]. One of these has furnished : Corynoides calicularis Nicholson D. angustifolius {Hall) Diplograptus foliaceus {Murchison) Lasiograptus mucronatus {Hall) the other : Nemagraptus gracilis {Hall) Climacograptus parvus Ifall Dicranograptus ramosus JIall Retiograptus geinitzianus Hall No outcrops of this zone in the Appalachian geosyncline south of those in New Jersey are positively known to the writer with the exception of that in Alabama found by Professor Smith. It is here, however, to be noted that the enigmatic species from Augusta county, Virginia, and Parrotsville, Tennessee, described by Emmons [American Geology, pt 2, p. 106 ff] as Monograpsus elegans, Cladograpsus dissimilaris, C. i n e q u a 1 i s and Diplograpsus ciliatus are more suggestive of the Normanskill zone than of any other, as already pointed out by Lapworth [1879, P-426] who recognizes Dicranograptus ramosus in one of the species of Cladograpsus. The " Monograpsus " is a Didymograptus and the Diplograpsus ciliatus a Glossograptus and probably identical with G. ciliatus \see ibid.'\. Collections of graptolites from Pennsylvania and Virginia sent to the writer by Dr Ulrich for inspection did not contain any elements of the 20 NEW YORK STATE MUSEUM Dicellograptus fauna. Of the Alabama graptolites [see list on p. 12] Nemagraptus gracilis var. surcularis, Dicellograptus cf. mensurans, Cryptograptus tricornis and Glossograp- tus ciliatus are forms occurring in our Normanskill shale; Crypto- graptus tricornis also entering into the next zone. Dicello- graptus s m i t h i is a close relative of D. sextans, another Normanskill form, indicating a transition of that species to Dicranograptus. Likewise Dicellograptus moffatensis var. alabamensis and D. foliaceus var. alabamensis are provincial representatives of species occurring in this horizon but also found in later beds ; the former is thus far known only from Great Britain, where it ranges from, the Llanvirn to the Hartfell beds, the other is a cosmopolitan form. A small Clima- cograptus which is nearest related to C . p u t i 1 1 u s may indicate syn- chrony with one of the later subzones of the Dicellograptus beds, and the large percentage of forms closely related to, but still distinct from Normans- kill species, is probably best explained as due to geographical or provincial separation. Following the slate belt northward into and through Vermont, no out- crops of the Normanskill shales have as yet been found in that State, but the presence of the zone with identical faunas in Canada for a long distance along the St Lawrence, made known by Lapworth [1887, Griffin Cove, Marsouin river, Little Mechin river. Cape Rouge, Quebec, Fox and Magdalene rivers] and Ami [1889, Island of Orleans, Etchemin river, Quebec, and Montmorency river, Quebec, etc.] leave little doubt of the continuation of the zone through Vermont ; and also the occurrence of an outcrop of the next graptolite zone near Lake Memphremagog, close to the Vermont and Canada boundary line points to the same inference. The apparent absence of the Normanskill shale from Vermont is quite obviously due to the stronger folding of the slate belt, possibly under the influence of the Adirondack massive in the west. This finds its expression in the greater vertical hight of the resulting mountain chains (Green mountains) and has led to a narrowing of the belts of shales and their GRAPTOLITES OF NEW YORK, PART 2 21 Stronger dynamic metamorphism ; all of these factors tending to obscure the possible outcrops of the horizon. The presence of Normanskill shale in northern Maine has been made known by Dodge [1890] and Ami has lately [1905J announced the occur- rence in New Brunswick of a graptolite faunule that belongs to this or the following horizon. West of the regions just mentioned the Dicellograptus fauna has not been observed again on this side of the Mississippi river. Its distribzUion in eastern North America may therefore be said to be restricted entirely to the Appalachian geosyncline and to some minor Atlantic embayments on the northeastern edge of the continent. In the Appalachian province again it is in the north strictly confined to the area which Ulrich and Schuchert [1902] have defined as the Levis channel, i. e. a narrow belt striking from New Jersey northward between the Quebec barrier and the Green moun- tain barrier to the St Lawrence, which it then follows to the St Lawrence gulf. The fauna entered this channel from the north and advanced, according to Ulrich and Schuchert, southward with the gradual submergence of the Appalachian valley trough, apparently never reaching beyond the present site of New Jersey. Its northeastern derivation is indicated by its northward connection with a sea which, as shown by the other embayments (Maine etc.), contained this fauna, by the European relations of the fauna to be noted further on and the apparent southward restriction of its area. The provincial differentiation of the northern fauna from that of Alabama would also seem to argue for an interruption of the connection in the middle third of the Appalachian valley trough, the northern fauna occupying the Levis channel or the northern third and the Alabama fauna all or a portion of the Lenoir basin or southern third. Whether this sup- posed invasion of the Dicellograptus fauna into the northern third was preceded by a draining of the Levis channel at the close of the Chazy with a subsequent resubmergence as Ulrich and Schuchert suggest, or whether it resulted from a separation of the southern and northern basins by a gradual elevation of the middle third would seem open to question. We 2 2 NEW YORK STATE MUSEUM had found [Mem. 7, p. 503] in the Deepkill graptolite faunas an element which strongly urged a closer connection of the same with the homotaxial Australian faunas, and for this reason inferred an open marine connection of the Levis channel southward or westward with the Pacific ocean — besides occasional openings of the basin to the Atlantic by means of the Newfoundland embayment — a view which has meanwhile received further support by the recognition of the presence of Mississippian (and Pacific) elements in the cephalopod faunas of the equivalent limestone beds in the adjoining Chazy basin. Since now the Upper Cambric Dictyonema shale, the rocks of the Deepkill horizons corresponding to the Beekmantown and those of the third zone, probably homotaxial with the Chazy, as well as the Dicellograptus zone, and, as shown further on also the succeeding zone, are coextensive in the Levis basin, the legitimate inference is that graptolitiferous beds were formed in that basin continuously from the Upper Cambric to late Trenton age with the exception of slight transgressions of the Missis- sippian sea in Trenton time, or in other words, that this basin, — or like physical conditions — ■ existed continuously through all these ages, its waters remaining always in connection with the Newfoundland embayment and gaining occasionally access to the Mississippian sea and thereby to the Pacific ocean. I believe that when all graptolite horizons of the Levis basin v/Ith their subhorizons shall have been distinguished and their proper succession recognized, a practically uninterrupted series of graptolite beds will become known extending from the Upper Cambric to the Utica invasion. An undubitable Dicellograptus fauna has been made known by Gurley from the novacuHte region in Arkansas [1892, where it was referred to the next zone, and 1896] which also has furnished a Beekmantown graptolite fauna. Although the material is not favorably preserved, the following forms of our Normanskill beds can be clearly recognized : Thamnograptus capillaris (Emmons) Didymograptus serratulus Hall Didymograptus sagitticaulis Gurley Nemagraptus gracilis (Hall) GRAPTOLITES OF NEW YORK, PART 2 23 Dicellograptus divaricatus {Hall) Cryptograptus tricornis {Carruthers) D. in tortus Lapworth Climacograptus bicornis Hall Dicranograptus ramosus Hall C. antiquus Lapworth ? D. nicholsoni var. parvangulus Gurley Glossograptus whitfieldi {Hall) Corynoides gracilis mut. perungulatus ' G. ciliatus Emmons ^°'"- Lasiograptus mucronatus {Hall) Diplograptus foliaceus Murchison Leptobolus walcotti" Ruedemann D. angustifolius Hall This association leaves no doubt of the homotaxy of the beds with the Dicellograptus zone of New York. But the black Arkansas shales also contain a few forms which by number and relative size are very prominent in the faunule and which do not occur in the Appalachian valley trough. These are : Dicellograptus divaricatus var. rigidus Dicranograptus nicholsoni var. arkansas- Lapworth ensis Gurley Diplograptus foliaceus war. trifidus Gurley^ The most noteworthy feature of these three forms is that they are identical with British varieties while they have not yet been observed in either eastern America or Australia. Dicellograptus divaricatus var. rigidus is a Glenkiln form, first described by Lapworth. D i c r . nicholsoni var. arkansasensis is, as noted in the description of the form here given, quite probably identical with an undescribed British variety of Dicr. nicholsoni that is figured in the MoitogTaph of British Graptolites, plate 25, figure ig, though the Normanskill shale of New York has also furnished a similar form in D. spinifer var. geniculatus. 'Overlooked in the original listing of the Arkansas graptolites. ^'Not listed by Gurley, but since described by the writer from the Normanskill shale of New York. 3 Dr Gurley lists also from Arkansas: Dictyonema o b o v a t u m n. sp., Lepto- graptus cf. annectans and Dicellograptus elegansvar. The first of these, based on a single type, I have been unable to find in the collection of the National Museum from Arkansas; the second identification refers to a very poorly preserved specimen and the third again has not been found. The last named species in England pertains to a higher horizon and its identification is doubtful \see Gurley 1896, p.296]. 24 NEW YORK STATE MUSEUM D i p 1 o g r a p t u s f o 1 i a c e u s van t r i f i d u s is either identical with or but little different from D. foliaceus var. calcaratus Lapworth. This evidence is, of course, by no means sufficient to infer a closer connec- tion of the Arkansas sea with the far-off British embayment of the North Atlantic, for it is to be noted that the forms mentioned are varieties of much varying and widely distributed species and may hence be convergent or parallel forms developed independently in different provinces ; and further Dicellograptus divaricatus and Diplograptus foliaceus var. calcaratus do not appear in Great Britain until the Hartfell shale stage. If they are not parallel but identical varieties, the suggestion could be made that the western sea stood in connection with the northeastern embayments of the North Atlantic sea by means of the Arctic ocean and the Baltic sea, the latter of which has also furnished Diplograptus foliaceus var. calcaratus (in Scandinavia)', the forms having orig- inated in the Pacific basin and reached the North Atlantic and Baltic basins later on. From collections made by Ulrich in the shales associated with novacu- ite in the Talihina formation of the Ouachita mountains in Indian Terri- tory, I infer that a horizon in close proximity to that of the Dicellograptus shale occurs there. One of the collections [loc. 240] contains: Dice!' )L;r;ii)tus divaricatus var. bicurvatus D. foliaceus var. (closely related to D. ^"'''- crassitestus nov. and probably Diplograptus foliaceus i]/«;T/«V6'« identical with D. trifidus Gurley) Climacograptus cf. antiquus Lapworth Another [loc. 240a] has furnished : Dicellograptus divaricatus var. rigidus Climacograptus bicornis var. tridentatus Lapworth Lapworth Dicranograptus ramosus Hall The occurrence of the variety of D i p 1 . foliaceus probably rep- ' See chart in part i of this monograph [Mem. 7, p. 488] which will, with slight changes, also serve to illustrate the present discussion in view of the continuous deposition of graptolitiferous beds during CHamplainic time in the same regions. GRAPTOLITES OF NEW YORK, PART 2 25 resenting t r i f i d u s , of C . cf. a n t i q u u s and of the variety r i g i d u s of Dicell. divaricatus suggests the homotaxy and provincial unity of the Arkansas and Indian Territory beds. Small faunules which contain elements of the Normanskill fauna have also been collected in Nevada by the geologists of the national government. One from the Silver Peak quadrangle contains : Nemagraptus sp. Diplograptus angustifolius Hall Dicellograptus divaricatus Hall D. cf. euglyphus Lapworth Dicranograptus furcatus Hall Climacograptus sp. The specimens are much distorted. Another from Belmont, Nevada [Wheeler Survey Rep't, 1875, v. 4, and Gurley, 1896, p.306] consists of Diplograptus foliaceus and Dicranograptus nicholsoni van w h i 1 1 a n u s . The pres- ence of the Normanskill zone or a closely preceding stage has long been known in the Rocky moitntains of Canada and in British Columbia. Lap- worth has recorded [1886] from Kicking Horse (Wapta) Pass, Rocky mountains : Didymograptus nov. aff. D. euodus Lap- Cryptograptus tricornis Carruthers worth Diplograptus angustifolius Hall Glossograptus cilia tus Emmons D. rugosus Emmons G. spinulosus Hall Climacograptus caelatus Lapworth and from the shales along Dease river, British Columbia [1889] : Diplograptus euglyphus Lapworth Glossograptus ciliatus Emmons Climacograptus c/. antiquus Lapworth Didymograptus c/. Sagittarius {Hall) Cryptograptus cf. tricornis {Carruthers) New form allied to Nemagraptus' ' Lapworth suggests that both the Kicking Horse pass and Dease river faunas may be a little older than the Normanskill fauna, mainly on account of the absence of the Dicran- ograptidae, Leptograptidae and Nemagraptidae. Since in America also the so called Upper Dicellograptus zone and the succeeding Utica shale are markedly free of these groups, the possibility has to be taken into account that they may be slightly younger than the typical Normanskill aggregation. At any rate it would seem to be giving an exagger- ated importance to this difference in faunal composition if they are correlated with the Chazy [Gurley, 1896, p. 304], for it must be noted that practically all elements of these faunules are present in our Normanskill fauna and they therefore can not be far removed from early Trenton age. 26 NEW YORK STATE MUSEUM While the locaUties of the Rocky mountain region demonstrate the presence of the Normanskill fauna in the easternmost part of the Pacific basin, Australia has also furnished ample evidence of the presence of this fauna in the southwestern part of the basin. T. S. Hall records the presence of the beds characterized by the Dicranograptidae from New South Wales [1902] and Victoria [1896, 1899]. From the former colony are cited : Dicellograptus r/. divaricatus /. tiall Diplograptus foliaceus Murchison D. cf. elegans Carruthers D. cf. whitfieldi J. Hall Dicranograptus zic-zac var. minimus Lap- Climacograptus bicornis /. Hall worth Glossograptus cf. mucronatus (/. Hall) Clathrograptus cf. geinitzianus (/. Hall^ From Victoria we find cited by the same careful author : Nemagraptus gracilis (/. Hall) D. elegans Carruthers Dicranograptus ramosus {J. Hall) Diplograptus pristis Hisinger D. nicholsoni Hopkinson Cryptograptus tricornis Carruthers Dicellograptus cf. sextans /. Hall Climacograptus bicornis J. Hall D. anceps Nicholson Lasiograptus sp. Associated with these forms are however new species, as Diplo- graptus thielei and Climacograptus wellingtonensis at Mt Wellington, which give the faunules a provincially different aspect. Turning now to the east side of the Atlantic basin, we find that the identity of a prominent graptolite zone in Great Britain with the Normans- kill shale was early recognized by Lapworth [1879 and 1880]. He states [1880, p. 198] of his "5. zone of Coenograptus gracilis Hall (or Dicellograptus sextans Hall)" which, by the way, is designated as the first of the " Upper Ordovician" : This is typically developed in the lower portion of the Glenkiln shales of the south of Scotland. It is the first of the Dicellograptidian zones, and is well particularized by the peculiar genus Coenograptus. Only a single Dichograptid (D . superstes Lapworth) survives. Dicranograptidae are abundant. Dicranograptus zic-zac Lapworth, D. formosus Hopkinson, Dicellograptus sextans Hall, D. intortus Lap- worth are peculiar, and several Diplograpti, such as Hallograptus bimucronatus Nicholson, H.? mucronatus Hall, Diplo- GRAPTOLITES OF NEW YORK, PART 2 2'] graptus whi tf ieldi Hall etc. This zonewas first recognized by Hall in the Normanskill beds of the valley of the Hudson. In Scania, Tornquist and Tullberg have succeeded in establishing a detailed succession of zones. One of the zones of the Middle Graptolite shales (zone h, of Coenograptus gracilis) contains near Fogelsong among others : Coenograptus gracilis Hall, Lasiograptu.s bimucro- natus Hall, Dicranograptus nicholsoni Hopkinson, Dicello- graptus cf. sextans Hall and several species of Diplograptus and Climacograptus. In France, Barrois [1892, p.145] has identified Diplograptus f o 1 i a c e u s and D. angustifolius among graptolites from the sand- stone of Saint-Germain-sur-Ille and tentatively referred the beds to the zone of Nemagraptus gracilis. The Bohemian graptolite shales have not furnished any characteristic forms of this zone. Lapworth's claim of the identity of the faunas of the Nemagraptus gracilis zone of Great Britain and of the Normanskill shale of New York is finding additional verification in the Monograph of British Graptolites now being published, in which some of Hall's species not before recorded from Great Britain are described ; and by the present publication in which the occurrence of an additional number of forms originally described by Lapworth from the corresponding British beds is recorded from New York. The graptolite lists of the horizon on both sides of the Atlantic are thus approaching to identity. Still, there remains a considerable number of species peculiar to each of the two regions and there exist also some dis- crepancies in the range of forms which call for explanation. Thus Amphigraptus divergens Hall, which is known here only from the Normanskill shale, is restricted in Great Britain to the zone of Pleuro- graptus linearis, which is the second of the zones succeeding that with Nemagraptus gracilis. Since it is a rather rare form in both the Normans- kill zone and that of Pleurograptus linearis, it is probable that its complete range is not yet known on either side. As in this instance, it would be in others perhaps rash to infer migrations from slight differences — unless 28 NEW YORK STATE MUSEUM supported by accumulative evidence — where one has to deal with faunas of obviously world-wide distribution. This does not exclude that there existed slight provincial differences between these pelagic faunas of the oceanic basins — a fact which we have already emphasized in the discussion of the distribution of the Deepkill graptolite faunas — and a possible concomitant exchange of forms that originated in the different basins. The Normanskill graptolite shales of the Appalachian geosyncline and those of the basins of Arkansas, Indian Territor)^ and of the Rocky moun- tain region are separated by the vast expanse of synchronous Trenton lime- stones extending across the intervening area. The Normanskill shale and the Trenton limestone not only approach so closely along the Quebec barrier as to come practically into contact, but they seem actually to overlap each other at times as indicated by the occurrence of Trenton conglomerate on Rysedorph hill and by certain observations of the writer in Saratoga and Washington counties. It would then seem that the Normanskill graptolite fauna of the Levis channel would have had, at least occasionally, ample opportunity to spread westward, across the barrier and it should be expected, in traces at least, in the Trenton limestone. The Trenton limestone has furnished the following faunule : 1 Dictyonema neenah Hall 4 Diplograptus amplexicaulis {Hall) 2 Dictyonema canadensis {Whiteaves) 5 Climacograptus typicalis Hall 3 Thamnograptus affinis Whiteaves Of these the first two are forms not represented in the Normanskill shale, the first is from the " Trenton limestone " of Wisconsin, the second, third and fifth are from the Galena-Trenton limestones of the Lake Winni- peg region which according to Whiteaves [1897, p. 135] "most probably represent the whole of the Utica and Trenton formations, inclusive of the Galena." This would explain the appearance of Climacograptus typicalis in the list. The Trenton limestone of New York has fur- nished the single species of Diplograptus amplexicaulis which occurs quite frequently in certain layers of the middle and upper Trenton at Trenton Falls and Middleville and is characteristic of a zone that is GRAPTOLITES OF NEW YORK, PART 2 2g younger than the Normanskill shale [see postea\. It can therefore be said that the Trenton limestone has thus far not furnished any evidence what- ever of the presence of the Normanskill graptolite fauna in the limestone- depositing areas of the epicontinental sea. 2 Magog shale (zone of Diplograptus araplexicaulis) Upper Dicellograptus subzone Gurley Lapworth [1887, p. 173] distinguished two subfaunas of the " Marsouin River or Normanskill fauna" of Canada, viz : Subfauna A The Coenograptus zone of Griffin Cove and the Marsouin river answering to the Middle Llandeilo beds of Great Britain, to the Glen- kiln beds of Scotland, etc. Subfauna B The Cove Fields and Orleans stibfaima ; apparently des- titute of Coenograptus gracilis, and answering to the highest Llandeilo or lowest Caradoc beds of England. Of the Cove Fields and Orleans subfauna, it is stated that it " shows evidence of a transition into the Utica-Lorraine Graptolitic fauna of the Mohawk valley, New York, and of Lake St John, Canada. The following species are cited from the two mentioned localities. 1 Cove Fields, near Quebec city : Diplograptus foUaceus Murchison var. Dicellograptus sp. D. amplexicaulis ? Hall Climacograptus two sp. D. truncatus (?) Lapworth C. bicornis Hall D. euglyphus Lapworth (?) Cryptograptus tricornis Carruthers Corynoides calycularis Nicholson Dicranograptus tardiusculus (?) Lapworth 2 Island of Orleans, near Quebec city : Dicranograptus ramosus (Hall) var. spino- C. bicornis Hall sus Lapworth Diplograptus foliaceus Murchison Climacograptus scharenbergi Lapworth Gurley secured a large collection near Magog' at the north end of Lake Memphremagog, at the boundary of Quebec and New Hampshire, 'A smaller list of the Magog fauna has also been given by G. M. Dawson [Geol. Sur. Can. Rep't, v. 7, 1894, Ap. 133J]. This is copied by Richardson [1902, p. 67] who figures a characteristic slab of this graptolite shale. 30 NEW YORK STATE MUSEUM and lists from this locality [1896, p. 296] which, as he states, furnishes the largest fauna of the subzone : Dicranograptus nicholsoni war. arkansasen- D. peosta mut. perexcavatus nov. ? sis Gurley D. truncatus ? Lapworth D. ramosus Hall Cryptograptus tricornis (Carruthers) Climacograptus caudatus Lapworth Lasiograptus mucronatus (Hall) id. var. laticaulis Gurley Dendrograptus unilateralis Gurley C. kamptotheca Gurley D. sp. C. oligotheca Gurley Dictyonema sp. incert. C. scharenbergi Lapworth Thamnograptus barrandi Hall C. wilsoni Lapworth Corynoides calicularis Nicholson Diplograptus foliaceus Murchison It will be noticed that these faunules observed in Canada are essen- tially relict faunules of the climacteric fauna of the zone of Nemagraptus gracilis. The Didymograptidae have vanished entirely and the Dicrano- graptidae almost ; only the long range forms Dicranograptus ramo- sus and n i c h o 1 s o n i are still observed, and the Diplograptidae can be said to hold now almost entirely the field with the genera Diplograptus, Climacograptus and Cryptograptus. The graptolite shales of New York or of any other part of the United States have not yet furnished a typical representation of this zone," but we have in this State several faunules which clearly are intercalated between the Normanskill and Utica shales and obvi- ously either represent fragmentary faunules of this zone or minor subzones of the same. As the most important of these we regard the shales zvith Diplograptus amplexua7ilis var. perteimis exposed in various localities (Watervliet arsenal etc., see N. Y. State Mus. Bui. 42, p.528) denoting a belt of rock that passes along the Hudson between the cities of Troy and Albany and is intercalated between Normanskill shales on the east and Utica shale on the west. Lapworth has also commented \op. cit. p. 172] on "the presence of a form identical with, or closely allied to, the G, amplexicaulis of ' Gurley thought at first to recognize it in the graptolite shales of Arkansas [1892, p. 403], but later [1896, p. 305] changed his view regarding the proper correlation of that fauna. GRAPTOLITES OF NEW YORK, PART 2 3 1 Hall" in the Cove Fields exposure and inferred that this occurrence might point to a homotaxy. with the lowest zones of the Black River or Trenton limestones. We have, in the paper cited before, adduced evidence to demonstrate the approximately middle Trenton age of this subzone. In some of the localities of the latter, as at Rusher's quarry at Troy, the form is associated with Corynoides gracilis. We would also refer here to the exposure of graptolite shale at the falls of the Hudson river at Sandy Hill, already known to the geologists of the first survey as Baker's falls and yet requiring more detailed study. Here a shale lying between Trenton limestone and Utica shale contains : Diplograptus amplexicaulis ( Hall) Corynoides gracilis Nicholson Climacograptus typicalis mut. spinifer nov. Trocholites aininonius Conrad Glossograptus (?) eucharis (Hall) By its lithologic aspect one would feel inclined to place this shale with the overlying Utica beds, but there is little doubt that the boundary between the Trenton limestone and Utica shale around the Adirondack plateau — or at least east of it — is by no means synchronous but shifting and that the shale in some places represents deposits of late Trenton age (and perhaps vice versa) and this faunule would serve to corroborate this view. A similar case pointing to the like view is that of a faunule collected by the writer at V^an Schaick island between Cohoes and Troy \sce Bui. 42, p. 524]. This consists of the graptolites : Chaunograptus ? rectilinea nov. Cryptograptus tricornis mut. insectiformis Diplograptus foliaceus mut. vespertinus nov. nov. Climacograptus putillus {Hall) These fossils are associated with Cameroceras proteiforme (Hall), Leptobolus insignis Hall and Schizocrania filosa Hall. It will be seen that this is in all respects a good Utica shale fauna, except for the occurrence of the distinctly gerontic mutation of Crypto- graptus tricornis. The latter species has never been observed in the Utica shale and its occurrence in this association indicates a transitional subzone between the Magog and Utica shales. 32 NEW YORK STATE MUSEUM The same can be said of another at present also isolated fauna that has been found by the writer at the power house below Mechanicville on the right bank of the Hudson river {see Bui. 42, 1901, p. 5 19]. It consists of a large number of brachiopods, moUusks and crustaceans partly denoting Utica, partly Trenton age, and the following graptolites : Corynoides curtus var. comma nov. Glossograptus quadrimucronatus var. ap- Diplograptus foliaceus Murchison proximatus nov. Climacograptus caudatus Climacograptus caudatus is restricted in Europe to the zone of Dicranograptus clingani, which corresponds to the Magog shale and lies between the zones of Nemagraptus gracilis (Normanskill shale) and Pleurograptus linearis (Utica shale). It has also been found in the Magog shale itself. Its occurrence in the Mechanicville shale together with a mutation that is restricted to this bed (Corynoides curtus var. comma) indicates a transitional subzone lying somewhere near the boundary of the Magog and Utica shales. We will for the present desig- nate it as the subzone of the two mentioned forms. The Climacograptus caudatus has also been found by the writer in shales dredged from the Hudson river at the city of Troy. The location of this latter shale indicates its stratigraphic proximity to the shales with Diplograptus amplexicaulis, our principal representative of the Magog shale. In Great Britain Lapworth [1880, p. 198] has distinguished 2, zone of Dicranograptus clingani Carruthers which follows that of Nemagraptus gracilis. It is in its turn succeeded by the zone of Pleurograptus linearis Carruthers, which roughly corresponds to our Utica shale \see postea\. By its relative stratigraphic position the Magog shale may, therefore, be expected to correspond to the zone of Dicranograptus clingani Carruthers. Although no complete fossil lists of the British zones, that would admit positive correlation are at hand, the presence, in the Magog shale, of such a form as Climacograptus caudatus that in Great Britain is restricted to this zone, leaves little doubt of their homotaxy. GRAPTOLITES OF NEW YORK, PART 2 33 TuUberg [1882, p. 18] has distinguished in Scania three subzones of that of Dicranograptus clingani Carruthers, the lowest of which alone car- ries Climacograptus caudatus while the highest one contains Leptograptus flaccid us, Diplograptus foliaceus and Cli- macograptus bicornis. It is, therefore, possible that his last subzone already corresponds to our lower Utica shale. Olin has also lately recorded [1906] the occurrence of Glossograptus quadrimucronatus in the Clingani zone in the neighborhood of Jerrestad in Scania and for this reason has suppressed Tullberg's zone of G. quadrimucronatus. It therefore becomes quite probable that the boundaries of our Magog and Utica shales do not exactly correspond to those of the zones of Climaco- graptus clingani and Pleurograptus linearis. 3 Utica shale (zone of Glossograptus quadrimucronatus and Climacograptus typicalis) The graptolite fauna of the Utica shale in New York and the adjoin- ing areas of Canada and Ohio consists of : Callograptus cotnpactus (Walcott) Corynoides curtus Lapworth Dictyonema arbuscula Ulrich id. var. comma nov. Mastigograptus tenuiramosus (Walcott) Diplograptus foliaceus mut. vespertinus M. simplex (Walcott) nov. M. gracillimus (Lesquereux) Glossograptus quadrimucronatus (Hall) M. arundinaceus (Hall) id. var. approximatus nov. M. circinalis nov. id. var. cornutus nov. Chaunograptus gemmatus nov. Glossograptus ? eucharis ( Hall) C. ? rectilinea nov. Climacograptus typicalis Hall Leptograptus annectans (Walcott) C. putillus ( Hall) Leptograptus flaccidus (Hall) C. bicornis Hall Pleurograptus linearis (Carruthers) Lasiograptus bimucronatus mut. timidus Dicranograptus nicholsoni Hopkinson nov. D. spinifer Elles 6^ Wood This fauna is markedly different from that of the Normanskill shale of New York and also well differentiated from that of the Magog shale. Its relict element from these preceding zones is very small. It consists of one 34 NEW YORK STATE MUSEUM species (Climacograptus bicornis) and a few mutations or dis- tinct derivatives viz, Leptograptus flaccidus heralded by L . f 1 a c c i d u s mut. spinifer, Dicranograptus nicholsoni with the prenuncial mutations diapason and parvangulus; D. spinifer, Diplograptus foliaceus mut. vespertinus, Lasiograptus bimucronatus mut. timidus. The common and characteristic graptolites of the Utica shale are all new forms; the most notable of these are : Corynoides curtus Lapworth G. ? eucharis (Hall) Glossograptus quadrimucronatus (Hall) Climacograptus typicalis Hall The last three cited graptolites the collector meets in almost every outcrop of typical Utica shale in both Canada and New York. Lepto- graptus flaccidus, Dicranograptus nicholsoni and Climacograptus putillus are very common in certain localities, but absent in others and apparently of more restricted horizontal and vertical distribution. Altogether, it is by no means to be assumed that the entire above cited assemblage of graptolites is found in every locality ; on the con- trary, the faunules of the localities are of so different aspects that the pres- ence of subhorizons, only to be established by careful stratigraphic work, can not be doubted. The following lists from some representative localities in New York State will demonstrate this fact. The Utica shale of the Mohawk valley, which from the presence of the type section in that valley is to be considered as representing the typical development of the formation, contains the following graptolites : Chaunograptus gemmatus nov. G. ? eucharis {Hall) Dicranograptus nicholsoni Hopkinson Climacograptus typicalis Hall D. spinifer Elles & Wood C. putillus {Hall) Corynoides curtus Lapworth Lasiograptus bimucronatus mut. timidus Diplograptus foliaceus mut. vespertinus nov. nov. Glossograptus quadrimucronatus {Hall) There are again distinct differences in the distribution of these forms recognizable in the Mohawk valley. Dicranograptus nicholsoni and D . spinifer have only been found in one locality, i. e. Fort GRAPTOLITES OF NEW YORK, PART 2 35 Plain.' The shales at Dolgeville, which are in the lower third of the Utica shale contain only : 'This is the " Dicranograptus ramosus," recorded by Professor Whitfield from the mouth of the Oxtungo creek near Fort Plain, N. Y. He cites from this locality [1877, p.19] Graptolithus (Monograptus) serratulus Hall, G. (Diplograptus) prist is Hall, G. (Climacograptus) bicornis Hall and G. (Dicrano- graptus) ramosus Hall; and infers from this faunule the homotaxy of the Normans- kill and Utica shales. The occurrence of Didymograptus serratulus has not been verified by later collectors and Lapworth remarks [1886, p. 171] that the form thus identified was possibly a Leptograptus. Likewise the list of Utica graptolites published by Walcott [1890, p.339] which is obviously based on Whitfield's original determinations has not been verified by the collections, at our disposal. The following species are named : 1 Didymograptus serratulus Hall 6 C. scalaris Hall 2 Dicellograptus divaricatus Hall 7 Diplograptus pristis Hall 3 Dicranograptus ramosus Hall 8 D. putillus Hall 4 Climacograptus bicornis Hall 9 D. mucronatus Hall 5 C. typicalis Hall Dr Gurley states in a manuscript note in regard to this list : " This list was compiled by me at Mr Walcott's request and to it I contributed my quota of errors. (Nos. 2 and probably 3, which latter is not otherwise accounted for.) The remainder were copied from a list in a previous paper by Mr Walcott, (The Utica Slate and Related Formations, 1879, p. 34, 35) which in its turn was compiled from the ' authorities.' " A similar faunule, viz : Climacograptus bicornis Hall Dicranograptus ramosus JTall Diplograptus mucronatus Jfall has been recorded by Beecher [1883, p. 78] from Black rock pond near Observatory hill, Albany, N. Y. This is associated with a fair-sized mollusk-fauna indicating very late Utican age. An inspection of the collection which is in the State Museum has shown that the graptolite faunule consists of : Climacograptus putillus {JIall) Glossograptus ? eucharis {HaW) Diplograptus sp. ind. (probably foliaceus) It is, hence, in full accord with the associated forms and the graptolite faunules of the neighborhood. 36 NEW YORK STATE MUSEUM Chaunograptus gemmatus sp. nov. Climacograptus bicomis Hall Glossograptus quadrimucronatus {Hall) C. typicalis Hall G. ? eucharis (Hall) while the shales in Flat creek at the south side of the Mohawk, belong- ing to the upper third afford: C. put ill us and Lasiograptus bimucronatus mut. t i m i d u s . The most peculiar distribution of all of these forms has Corynoides c u r t u s which is common in the outcrops of the Appalachian trough \_see postea\ but in the Mohawk valley has been traced only a short distance west- Ward (to Amsterdam) and has never been seen by the writer in collections of the Utica shale of the middle and upper Mohawk valley, the outcrops west of the Adirondack region or of the Cincinnati and Maquoketa shales. The faunule of Holland Patent, which has become known by Walcott's investigation [1879] has again a different aspect. It consists of : 1 Callograptus compactus (Walcott) 8 Glossograptus quadrimucronatus ( Hall) 2 Mastigograptus tenuiramosus {Walcott) 9 G. ? eucharis {Hall) 3 M. simplex (Walcott) 10 Climacograptus typicalis Hall 4 Leptograptus annectans (Walcott) 11 C. putillus (Hall) 5 Pleurograptus linearis (Carruthers) 12 Lasiograptus bimucronatus mut. timi- 6 Dicranograptus nicholsoni Hopkinson dus nov. 7 Diplograptus foliaceus mut. vespertinus nov. Nos. I, 3 and 5 of this list have thus far not been recorded from any other locality in the United States ; the two species of Mastigograptus are also known from Canada ; and Pleurograptus linearis, which is known to me only in a single specimen from Holland Patent, marks a zone in the Hartfell shales of Scotland and Scania. It is probably proper to consider this faunule as typically representing the European 2one of Pleurograptus linearis [see postea\. The Utica shale faunules of the Appalachian trough in New York form a group by themselves' by the common occurrence of Corynoides ^ They have been fully cited with their associated nongraptolitic forms by the writer in N. Y. State Mus. Bui. 42, 1901, p.sig ff. GRAPTOLITES OF NEW YORK, PART 2 ■^'J c u r t u s in nearly all of them. One of the most important of these faunules is that from the Rural cemetery near Albany. It consists of : Mastigograptus circinalis sp. nov. G. ? eucharis (Hall) Corynoides curtus Lapworth Climacograptus putillus ( Hall) Glossograptus quadrimucronatus var. cor- nutus fwv. This interesting faunule stands apart from all others by the peculiar and striking variety of G. quadrimucronatus and by Mastigo- graptus circinalis, two forms that have not been found elsewhere, while on the other hand Climacograptus typicalis is entirely absent. It most probably represents a separate subzonal association. The other localities as e. g. the Penitentiary at Albany and Black creek at Voorheesville have furnished : Corynoides curtus Lapworth Climacograptus typicalis Hall Glossograptus quadrimucronatus {Hall) C. putillus (Hall) G. ? eucharis {Halt) This faunule can be considered as a typical one for the Utica shale of this belt. The transition beds from the Trenton limestone to the Utica shale exposed at the lake shore at Panton, Vt., consisting of alternating lime- stones and shales which contain in the limestones a Trenton and in the shales a Utica fauna, have furnished to the writer : Corynoides curtus Lapworth Climacograptus putillus ( Hall) Glossograptus quadrimucronatus ( Hall) Lasiograptus bimucronatus mut. timidus G. ? eucharis {Hall) nov. These forms are among the earliest of the Utica graptolite fauna. Climacograptus typicalis seems to come in a little later. A tunnel of the New York and Lake Erie Railroad being constructed at Otisville through the Shawangunk mountains at the New York and New Jersey boundary has furnished to the writer from shale, directly underlying the Upper Siluric Shawangunk grit, besides specimens of Schizocrania filosa Hall: 38 NEW YORK STATE MUSEUM Glossograptus quadrimucronatus {Hall) C. typicalis Hall var. C. putillus (Hall) Climacograptus bicornis Hall This occurrence indicates the continuation of the Utica shale belt of the Hudson river valley into New Jersey, although the presence of the Utica shale fauna has not yet been recorded from the " Hudson River slate" of that State. Collections made in Pennsylvania by Dr Ulrich, which I have had occasion to see, leave no doubt of the farther extension of the Utica shale into that part of the Appalachian trough. The extensive Utica shale exposures of the Lake Champlain region are, as Professor Perkins correctly remarks, singularly barren in fossils and especially in graptolites. The long continuous exposures of Grand isle yielded to the present writer only a few specimens of Climacograptus typicalis.' On the New York side of the lake only a few small patches of Utica shale remain, the most notable of which are those near Addison Junction and Rouse Point. In Canada the faunas of the various localities have been carefully listed by Ami in his paper on the Utica Terrane in Canada [1892]. Glossograptus quadrimucronatus, G. ? eucharis and Leptograptus flaccidus appear in nearly all of the lists ; besides M as t igogr ap t u s simplex, Climacograptus bicornis ?, C. scharenbergi ?, C. sp. and Diplograptus pristis. We have had occasion to observe the presence of both Climacograptus typicalis and C. putillus in Canadian Utica shale and since Ami comments on the difficulty of determining the Climacograpti \ibid. p. 16], it is quite obvious that his tentative identifications refer to these two species which, at that time being not yet described and known only from Hall's enlargements of fragments of the rhabdosome, were not easily recognized. Mastigograptus tenuiramosus I have seen in Canadian specimens sent me by Professor Whiteaves. 'Professor Perkins [1904, p. 106] records Climacograptus bicornis and Diplograptus pristis from the Utica shale of Grand isle. GRAPTOLITES OF NEW YORK, PART 2 39 The collection from the Utica shale of Cincinnati kindly loaned to me by Dr Ulrich contains : Dictyonema arbuscula ( Vlrich) Climacograptus typicalis UaU Mastigograptus tenuiramosus iy/alcott) C. putillus {Hall) M. gracillimus (Lesquereux) Lasiograptus bimucronatus mut. (Diplo- Chaunograptus gemmatus sp. nov. graptus whitfieldi et spinulosus auct.) Leptograptus annectans {Walcott) Dicranograptus nicholsoni Hopkinson (Dicr. ramosus auct) It will be observed that this is in all respects a true though greatly depauperated Utica graptolite fauna. Especially notable is the absence of Glossograptus quadrimucronatus, G. ? eucharis, Climaco- graptus bicornis and of the later mutation of Diplograptus f oliaceus. According to Nickles [1902, p.68 ff] Mastigograptus gracillimus {Lesquereux) C. putillus {Hall) Climacograptus typicalis Hall range through the formation while Mastigograptus tenuiramosus {Walcott) Lasiograptus bimucronatus mut. timidus Dicranograptus nicholsoni Hopkinson nov. are restricted to the lower Utica and Dictyonema arbuscula to the middle third of the formation.' On the other side of the Cincinnati geanticline or parma, in Wisconsin, Minnesota, Iowa and Missouri, the Maquoketa shale is currently considered as the equivalent of the Utica shale of New York. Winchell and Schuchert [1895, p.Si ff] cite Diplograptus pristis ? (Hisinger) Hall and 'Ulrich and Schuchert [1901, p. 645] consider the middle and upper Utica of Nickles's Cincinnati section as equivalent to the Frankfort shales, "the typical Utica barely reach- ing that point, though something like 300 feet thick in northwestern Ohio." The presence of Climacograptus typicalis and C. putillus in these beds does not seem to support this view, since the former is not known here to pass beyond the Utica shale and the latter only enters the lower or transitional Frankfort beds. It must, however, be conceded that the graptolite faunas of the Frankfort and Lorraine shales in New York are still very imperfectly known, and that both forms may possess longer ranges than hitherto observed. 40 NEW YORK STATE MUSEUM D , p u t i 1 1 u s Hall from it. The former determination refers quite obvi- ously to specimens of Hall's species D . p e o s t a, originally described from this region but not figured until lately. We have before us a collec- tion from the Maquoketa shale at Spencer, 20 miles south of St Louis secured by Dr Ulrich and containing a small new Climacograptus (C, u 1 r i c h i ), related to C . t y p i c a 1 i s ; and representative collections from the better known graptolite localities in Minnesota, Wisconsin and Iowa, kindly secured for us by Professor Sardeson. These indicate the presence of a slightly greater faunule than has hitherto been recorded. One of the beds of Maquoketa shale contains a small graptolite in such numbers that it has been distinguished as the Diplograptus bed [see Sarde- son, 1897, p. 24]. Specimens from the exposure of this bed at Graf, la. contain D. peosta in plastic preservation, exactly like Hall's type of that species (from Maquoketa creek) in the American Museum of Natural His- tory. Fragments of the Diplograptus bed at Elgin, la. contain Glosso- graptus ? eucharis in great number and typical development and a few specimens of G. quadrimucronatus. The well known locality at Granger, Minn, furnishes in Diplograptus bed no. 11 : Diplograptus peosta Hall, the prevailing Lasiograptus bimucronatus mut. timidus form nov. Climacograptus putillus ( Hall) A few rock specimens from the Triplecia bed (=no. 10) near Wykoff, Minn, contain Diplograptus peosta and others from the Leptaena bed (=no. 13) Glossograptus quadrimucronatus. The complete graptolite fauna of the Maquoketa beds would hence consist of: Diplograptus peosta Hall C. putillus (Hall) Glossograptus quadrimucronatus {Hall) Lasiograptus bimucronatus mut. timidus G. ? eucharis (Hall) nov. Climacograptus ulrichi nov. On the whole, this association can properly be considered as a frag- mentary Utica shale fauna, but it is to be noted that the most frequent form. GRAPTOLITES OF NEW YORK, PART 2 41 Diplograptus peosta Hall, is in New York State not a Utica but a Lorraine fossil and that the others are species which here apparently range through the greater part of the Utica shale and partly beyond it. It is therefore very probable, from this evidence at least, that the Maquoketa shale is equivalent only to the last part of our Utica shale and to a part of our Lorraine. In this connection it is also important to note that the characteristic Utica shale graptolite, Climacograptus typicalis, which in its typical expression is not present in the Maquoketa shale, is reported by Winchell and Schuchert \op. cit. p.82] from the Galena lime- stone at Mantorville and Weisbach's dam near Spring Valley, Minn., and listed by Winchell and Ulrich \ibid. p.CXI] as occurring in the Fusispira and Nematopora beds, i. e. at about the middle of the Galena dolomite. Since this form has not yet been observed below the Utica shale in the east, its earlier occurrence in the west suggests either that it migrated into the Utica shale region of the east from the northwest, which is contradictory to other evidence or that some of the upper Galena beds may be already of the age of our Utica shale which though apparently not supported by a comparison of the Galena and Utica litoral faunas is possible in view of the very different facies of the two and the corresponding differences in the faunal aspects. In such a case, it would be just the pelagic forms such as the graptolites from which we would expect positive evidence of synchrony. Finally, the deposition of graptolitiferous shales seems also to have persisted into Utica time in the basin oi Arkansas, where already the Beek- mantown and Trenton graptolite zones are represented ; at least, a slab of the National Museum collection [loc. 1243B] with Corynoides cf. curtus Lapworth, Climacograptus typicalis and Diplo- graptus sp. and the abundance of Climacrograptus putillus in another locality [Center sec. 13, 35, 17W] would suggest such an occur- rence; and Dr Ulrich has even found in Indian Territory \see pos^ea'j.a. small graptolite fauna in shales overlying a bed with a Richmond fauna. In Europe we find the equivalent of the Utica shale in the zone of Pleurograptus linearis. As stated before, it is probable that the two are 42 NEW YORK STATE MUSEUM not exactly equivalent, Glossograptus quadrimucronatus, for instance, appearing already in the preceding zone of Climacograptus clingani. The time for exact correlation has, however, not yet arrived ; its prerequisites are a more detailed zonal study of our graptolite shales, notably the Utica shale, and the publication of complete fossil lists from the European graptolite beds. The zone of Pleurograptus linearis is best developed in Scotland, where it abounds in Leptograptidae, and also well known in Scania [Lapworth, 1880, Olin, 1906]. Glossograptus quadrimucronatus is a prominent form of the zone in both Britain and Scandinavia. The Utica shale is the first Champlainic graptolite shale which posi- tively trangresses the western boundary of the Levis channel of the Appa- lachian geosyncline in New York and not only extends the full length of the Champlain basin connecting northward with the Ottawa basin, but also passes in a broad belt through the Mohawk valley around and over the south side of the Adirondack plateau and through the Black river basin on the west side of the Adirondacks, to Lake Ontario. In Canada, according to Ami [1892, p. 17], the Utica shale is first met with north of the Island of Anticosti. "The Utica terrane occupies a more or less narrow and con- tinuous belt along the north shore of the St Lawrence from Cape Tour- mente, below Quebec, to Montreal whence the belt trends to the south, . . . crossing the boundary line." An interesting outlier is found far to the north of this belt in the Lake St John region or Upper Saguenay district. It is from this area that Hall's types of Glossograptus quadri- mucronatus, G. ? eucharis and Leptograptus flac- cidus, three of the most characteristic fossils of the Utica shale, have come. Another outlier is found in the Ottawa basin. South of the interna- tional boundary the Utica shale follows the Champlain basin appearing in several small outliers on the New York side and in a broad belt on the Ver- mont side, especially on North Hero and Grand isle. At the upper Hudson the belt of outcrops divides, one branch continuing southward along the GRAPTOLITES OF NEW YORK, PART 2 43 Hudson and bending southeast with the whole belt of " Hudson River shale " north of the Highlands, its last outcrop being observed close to the New Jersey boundary. It probably continues in the Appalachian trough into Pennsylvania and Virginia. The other branch skirts the Adirondacks in the Mohawk valley and on their west side, disappearing beneath Lake Ontario to reappear in the Province of Ontario, crossing the same to Col- lingwood, "where it disappears beneath the waters of the Georgian bay and continuing north and west strikes numerous points, capes and islands about the great Manitoulin island dying out to the west and overlaid by newer and overlying formations." The reappearance of Utica shala in the center of the Cincinnati geanti- cline at Cincinnati, and its tracing through Ohio (by well borings) demon- strate that the narrow belt of outcrops above delineated, does by no means indicate the whole distribution of this widely extended shale formation. The St John and Ottawa outliers show that the shale extended far on the " Canadian shield " and an outlier at Wells in the southern Adirondacks demonstrates that the Utica sea also swept at least a part of that plateau. The facts of this wide overlap combined with the shaly nature of the rocks and their greatly varying, often considerable thickness indicate that the Utica formation is the result of a great transgression of the sea brought about by a general depression of the northeastern part of North America. The transgressing sea came in from the northeast and brought with it a fauna with decided Atlantic elements ; and currents developed which assisted in spreading the shales and the immigrating fauna far into the epicontinental sea.' The facts of this transgression and enlargement of the northeastern communication with the Atlantic would seem to aid in explaining the differences between the graptolite faunas of the Utica shale and the under- lying beds, and certain peculiarities in the areal distribution of some of the Utica shale graptolites as Corynoides curtus, Glossograptus ■" See Matthew, Roy. Soc. Can. Trans. 10 : 15 ; Ruedemann, Amer. Geol. 1897. 19: 367-91 ; 21 : 7S-8i ; Ulrich & Schuchert, N. Y. State Mus. Bui. 52. 1902. p.642. 44 NEW YORK STATE MUSEUM quadrimucronatus and Leptograptus flaccidus. The first named graptolite fails to appear in the south and west of the Adirondacks ; G. quadrimucronatus attains its largest size in the St John basin and is in New York represented in smaller forms and L. flaccidus which appears in prenuncial forms in the Normanskill shale and disappears in the Magog shale, did not, in the Utica age, again reach New York while it is abundant in Europe, the St John basin and lower Canada. The Cincinnati graptolite fauna when compared with that of New York appears so depauperated that it is easily recognized as being far away from the center of distribution. It follows as a corollary from the conclusion of the transgression of the Utica shale and fauna from the northeast, that the boundary between the Trenton limestone and Utica shale is not a plane of synchrony in the State. The alteration of the Trenton into the Utica condition took place very gradually ' and proceeded slowly westward. Sensitive horizon markers, such as the graptolites, may therefore with progressing refinement of the subdividing of the zones well be expected to fix the exact zonal planes of the boundary line between the Utica shale and Trenton limestone in the different regions by the establishment of the western extension of each subzone. The earlier subzones, for instance that of Mechanicville with Corynoides curt us var. comma and Climacograptus cau- datus did, in the writer's opinion, extend but a very short distance west beyond the margin of the Appalachian trough and are overlapped by younger zones farther west. The before mentioned restriction of the areal distribution of Corynoides curtus to the lower Mohawk valley may 'This is indicated by numerous alternations of Trenton limestone with shales, as emphasized by Ami in Canada, by Perkins in Vermont and by Walcott [1879], Gushing and the writer [1897] in New York. Perkins [1904, p. 107] has described the presence of an intermediate shale with both Trenton and Utica fossils from Grand isle ; the writer found an alternation of limestone and shales, the latter with typical Utica graptolites, at Panton, Vt., and Gushing has distinguished the passage beds as a separate unit on the Little Falls sheet. GRAPTOLITES OF NEW YORK, PART 2 45 be also due to the greater age of the eastern Utica beds and their absence farther west, where they are probably represented by the lowest Trenton limestone. 4 Lorraine beds The Lorraine beds, which term is here used to include both the Frank- fort and Lorraine shales, are according to their graptolite fauna but little differentiated from the Utica shale ; they contain little more than a relict fauna of the Utica shale and are bound closely to it by transitional beds. The fauna of the Frankfort shale (subzone of Glossograptus quadri- mucronatus viut. postremus) as represented at Waterford and Mechanicville, consists of : Corynoides curtus Lapworth Glossograptus quadrimucronatus wm<. post- Diplograptus foliaceus mut. vespertinus remus nov. '^0^- Climacograptus putillus {Hall) The fauna of the Lorraine shale (subzone of Diplograptus foliaceus mut. vespertinus and Diplograptus peosta) consists in the Black river region of : Diplograptus foliaceus wMi. vespertinus MOW. Diplograptus peosta Hall The faunule of the Frankfort shales is characterized by the gerontic character of its mutations of D iplograpt us foliaceus and Glosso- graptus quadrimucronatus as being in a decadent stage ; that of the Lorraine beds of the northwestern part of the State possesses in Diplograptus peosta a new element. This species has been here currently identified with Diplograptus amplexicaulis' and it seems indeed to be in its habit and character essentially a smaller D . amplexicaulis. If the latter is the correct conception, this form would constitute, another case of the reappearance of Trenton forms in the Lorraine beds. The Lorraine shale, the typical exposure of which is in the Lorraine gorge south of Watertown in northwestern New York, is restricted to the * James, Walcott, Whitfield and Hovey, Ruedemann, see under D . peosta. 4.6 NEW YOEK STATE MUSEUM west side of the Adirondack plateau. It extends in the Mohawk valley only as far east as Rome. The Frankfort shale is apparently absent in the Champlain basin, but forms south of it a belt that crosses the Mohawk river at its mouth and thence extends westward on the south side of the Mohawk valley ; and southward, disappearing under the Helderbergs but probably reappearing in the southern continuation of the Appalachian slate belt in New Jersey and Pennsylvania. From this distribution of the rocks the inference would suggest itself that the region east of the Adirondacks had become drained during Frankfort time, and the former marine connection of the Appalachian trough and western sea with the Atlantic basin had been interrupted there, the sea gradually withdrawing until at the beginning of Lorraine time it extended only as far as Rome. But it is quite as possible that the Frank- fort beds of the Champlain region, being the last deposited and not pro- tected by being infolded with the other rocks as in Saratoga and Albany counties, have all been abraded again. This view finds support in the fact of the presence of Lorraine beds directly north of the Champlain basin, south of Montreal, with a thickness of several hundred feet and a char- acteristic fauna \^see Ami, 1900, p. 159], and in the great thickness of the formation in Albany and Schenectady counties. 5 Zone of Dicellograptus complanatus Lapw. Dr Ulrich's collection from Indian Territory contains a small graptolite faunule. It was obtained in the Sylvan shale of the Arbuckle mountains, and consists of Dicellograptus cf. complanatus Lapworth Climacograptus mississippiensis nov. Diplograptus crassitestus nov. Dr Ulrich informs me that this interesting association overlies a Rich- mond fauna. It is hence probably representative of the youngest Lower Siluric beds of North America. This inference is to some extent borne out by the graptolitic evidence, notably by the presence of specimens of a Dicel- lograptus which, as far as their somewhat fragmentary character permits GRAPTOLITES OF NEW YORK, PART 2 47 of a conclusion, is identical with D . c o m p 1 a n a t u s. The latter grap- tolite characterizes in Britain and Scandinavia the zone above that of Pleurograptus linearis. Lapworth [1880, p. 298] describes this zone as follows : Zone of Dicellograptus complanatus, Lapworth — The strata that lie between the zone of P. linearis, Carruthers, and the summit of the Ordo- vician system form in south Scotland two very distinct zones, though few Rhabdophora have yet been described from there. The lowest zone is that of Dicellograptus complanatus, Lapworth which contains but few peculiar forms in addition to its characteristic species. It is recognizable in the same stratigraphical position and affording the same fossils at Moffat (Barren Mudstones), at Girvan, in County Down, at Rostanga in Scania in the lower part of the Trinucleus schist, and in Westrogothia. If our determination of this graptolite is correct, the beds in Indian Territory containing it would properly be correlated with this European zone. Diplograptus crassitestus Is a species with peculiarly coarse structure and reminds in its entire habit most strongly of D. tr if id us Gurley, a form already occurring in the same region in Normanskill time. Climacograptus mississippiensis is distinctly a later derivative of Climacograptus typicalis and points to the rela- tionship of this zone to the preceding one. It is a close relative or vicari- ous form of C. latus \see under C. mississippiensis] which is found- in the highest Champlainic (Ordovicic) graptolite zone of Europe, that of Dicellograptus anceps. A summary of the analysis of the graptolite zones of the upper part of the Champlainic and their correlation with those of Europe is found in the correlation table at the beginning of this chapter. 48 NEW YORK STATE MUSEUM u E H a. o > o Q O < a. < c u u a. a 3 .J o a u in E U O U3 tn Q MS g= < o £ H u. o z o H f- m E H u. o u CO < (- o z SNOioan >iaHxo vnvHxsnv VIAVNIONVOS < < a^vHS aiaax^vH aivHS Nai:HNaao snoaNvaaaDsiw SVSNV5IHV NOIOaa IXVNNI3NI3 XX X VMvavav vavNVD X X anoA AvaN: X X X X X xxxxxxxxxx aivHS aNivanoi aavHS VDixn. aivHS ooovw aavHS t:ii:hsnvwhon aNOxsawn NOXNanx o c "73 ^ > s 2 ^ rt H o 0) (U m ^ Pi D ^ — ' o .2 S =3 ro 1 — I a, c i^ ?;K d C O "J^^ O ■!-> U I— 1 . E 3 ^ -^ S C 3 o o . O U3 cij •2 M ni 3 o ■^'^ = " O 5 hD 3 CIS 3 S nj in M '^'J °S (11 r-t TO V- -H C oi oi p see (U 3 T3 O o 3 SO o o 4J •rl ..4 Ml — ' !:z: ni « XJ en t/i wk 2 2 S CJ (i; Q Q d Q O Q H S § § S' ^ 6 U &; O Q Q ni t. C 0) •r^ 3 >H oi ^. O .00 Os O •-< n ^ GRAPTOLITES OF NEW YORK, PART 2 49 V :z; X X X X XXX X y. xxxxxxxxxxxxx X X y, X X y. y. X X y. X • ■ y. y. X y, ■ X X X X X X X c B V Id iH l-l l-C O O >-, O h O >H >H ^^ o o 1-. o o CJ u c >^ a S'S Sf^ as O 3 -■ o a 1-1 3 h, >:: ?i .■" Ij 4_, .J-. • ■—I rn a. £/: n\ -M Ui C) c« a; > (-1 CC rt hJhJ mvo CJ 01 V ^ ri f5 U w C_) oJ (U — ^ d) D > (H, G •Ji; M •^ -a 3 r-J Cfl « CTJ ■4-J :j '^ 'm >^ PS 3 T3 Sag CO Ph l> > CJ CJ U rt n1 cvi ;-! M ^ H M bfl fcJ3 OJ , , 'Z'Z.'Z,'^ OS # ft ni e a O u- — ■ o Id :=: S « 2 rrt -o S Pi w > b 2 3 ii rQ Gj O J-* o ■ T3 : § :=; o u en o O .- O- s= --i I— I ^ ■ i=a g 4J "O ni ►in -; (U 4J .^ O t: 3 O 1- CJ IH >< !-. O lO' CrP^W: u) ; > t3 ^ •- (U t/l IJ -' t/5 d ■- • t^ >< X o d B 'd > > > > '-5 '-5 t- v^ tn TO cd —' --^ >• >■ S ^ '■5 -S .S .^ tn ^ aj 0) O. ij ^4 crt CTl > > w ni .^ ■ Ci-Td ni rt oi ' > > O c c ri S V 3 P^ ; o 4i !> ri P^ ■ffi S ■" - •7° u-" IJ ri Cm;— 3 .ii ^ bO td bfl uo c/: c/] w: 3 t^ ri M- - > ° ^- X- ^ j:; o o o *-• c G c > «^ > ii ^ . ri 3* G C O ri ft ft 3 t^ 02 en ^^ ' S ° ' a; en M ri ro -t- m^ r— CO -t-t-t-h-t-f-t-t C-bD O . ON O '-' f^ ^ "f" iJ^^ r^oo ON O '-' N ro -t in :^:ziz"QOQPCCQdcdGdGdGGCGC;GCCQQOQ 50 NEW YORK STATE MUSEUM a Z 3 U r H u. o o u > o o c< o < a. < E u B^ u B. 0. 3 cu _] o s ? H g u. ■"" o w UJ t5 j« o H a. < a lU E H u. o z o p 3 oa H t/3 a E (- u. o u ,J < H 0. o z > SN0I03X HaHXO a o o a? in ■" . ^ 5 fe O ^ C ^ >, O ^ ' vnvHxsnv VIAVNiaNVOS <: <; STVHS ^^adxavH aavHS Nai'HNaao sno3Nv^^a^SIlM X X svsNVJiav NOIOaH IXVNNIDMID VIMVaVTV vavNvo XXX 'X'aoA MaN X x >< >^ XXX 3TVHS aNIVH'aOl aTVHS voi.m o o o o o o aTVHS oooviM aTVHs tii:hsmvimhon O V 3N0xsawn noxn3hx a S to ■9.-^ '-'Or, g '^ *-* 05 tn = 33 c 0) ; 1 T-l n! 3 K a, Pi:; « t/3 ' ' 1 aj p > = t/: O nj >-. 1-, 1-3 3 n! ri ni ai > > > > 3 ^ C t/5 ^- ^ v en & 3 •13 "o C (3 ni S UJ -a aj 3 ^p4 ^ 3 o aj f=^ s '^ bO o o o o o o >- ■^-H ^4-( ■-*-< U-l "-W t+H O &^bO S S G rt ^ ^ be bo O 3 3 1) 1> "U &t (J E w O 3 ^ c „ S '3 1) " — ' 3 „ " O rt ,§ 3 X +-■ O 3 Oh >-, CI, o -o -; >- b o a > 'O -0 13 rt ni 3 3 QGQ O OOOOO On O tH «^00 CO 00 00 00 00 00 GRAPTOLITES OF NEW VORK, PART 2 Kl I /a o ^W S pq r, cfi »H •— « CU o 0) (U ™ en .S fi^ (L) C ^ CI fl g-c 1—1 COO ■SoTsm .t2 c 1) >^L~ ;2; ddd 00 o o 00 00 Oi 3 S nJ P, P, Clj u u u u cJ u J d ""^ o rj ro ^ loO r^oo On O a\ONasa\OsasCNO\M ooooooooo V 4) ■Sin ^« ." ^•r 4) = c^ - ^ n'S P-.S S « ° - (inj: bfl u c "biS 52 NEW YORK STATE MUSEUM SYNOPTIC TABLE OF THE DISTRIBUTION OF THE QRAPTOUTES OF THE SILURIC (ONTARIO OF THE UNITED STATES 1 Dendrograptus rectus Ruedemann 2 Dictyonema pertenue Foerste D. scalariforme Foerste D. retiforme Hall D. gracile Hall D. polymorphum Gurley MS 7 D. SLibretiforme (Spencer) 8 D. areyi Gurley MS 9 Desmogra])tuspergracilis (Hall & Whitfield) 10 Cyclograptus rotadentatus Spencer 1 1 Ptilograptus hartnageli sp. nov J 2 Inocaulis plumulosus Hall 13 I. divaricatus Hall 14 Acanthograptus walkeri Spencer 15 Cactograptus crassus Ruedemann 16 Palaeodictyota anastomotica (Ringueberg) 17 P. clintonensis Ruedemann 18 P. bella(Hall) 19 P. bella mut. recta- Ruedemann 20 Chaunograptus novellus Hall 21 Climacograptus scalaris (Hisinger) var. an- nulatus Ruedemann 22 Monograptus clintonensis (Hall) 23 M. priodon Bronn mut. chapmanensis Rued- emann 24 Cyrtograptus ulrichi Ruedemann 25 Retiolites geinitzianus Barrande j Note on terminal spines of Climacograptus bicornis Perhaps the most striking objects among the Normanskill graptolites, especially those from Glenmont near Albany, are the appendages of the sicular end in Climacograptus bicornis Hall. They present at first sight an almost bewildering variety of forms and all possible modi- fications of a single pattern. They all occur in one and the same horizon GRAPTOLITES OF NEW YORK, PART 2 8 1 and a little further study shows that even the most extreme forms are con- nected by an infinite number of transitional stages. It thus becomes apparent that we have here one compact phylogenetic group of no more than specific rank which, however, with a sudden outburst of variability develops along various lines, some of which diverge widely enough to have been designated as different varieties. In the succeeding Utica formation the species, or a mutation of it, per- sists, but the wealth of appendical forms has disappeared, and the onto- genetically earliest and phylogenetically oldest plain, double-spined form alone survives. I have here arranged a number of the most characteristic forms from the Normanskill shale on plate A to bring out synoptically the probable lines of development of the varieties. The elements of these modifications are the two spines, arising from the outer walls of the first two thecae, the virgella or principal spine of the sicula and the alate extensions of the spines. The simplest stage is the bicornis stage, occupying the lowest tier of the plate. In this only the two lateral or thecal spines are developed. The young of all the other varieties pass through this stage and the form shown by most of the young and the Climacograpti of the preceding horizon is to be considered as the most primitive. This is the one represented at the base of the plate, with two slightly curved, widely diverging thin spines. These appendages then begin to vary by (i) the degree of their diverg- ence and (2) their curvature. They become either straight as in the lines g and e, recurving as in f or curving inward and becoming semilunar as in the other lines a-d. The degree of divergence of the spines may be influenced by the direction of compression and some of the apparent modification is hence due to this cause. Since with the exception of the line a, in which the prongs have been subparallel, the angle of divergence has not been given any importance and the appendages would naturally tend to settle on this flat side, the direction of compression is evidently a factor that can be here neglected. 82 NEW YORK STATE MUSEUM The simple needlelike spurs of the earliest bicornis stage show a tendency to develop wings on their back. In most specimens these wings grow most rapidly at the base of the spines, as in the lines a, b, d, e, f of the plate, whereby in the inward curving varieties a crescent form arises \_see 9, .12], in the straight spined forms appendages similar to mackerel- tails [13] and in the recurving forms appendages reminding one of lumbermen's hooks [14]. By continued growth of the wings the group of forms is originated, which has been designated as Climacograptus bicornis var. pelt if er [tier II of plate A]. A glance at the plate shows that here again all of the bicornis varieties occur, namely forms with crescent- shaped spines (b), with straight diverging spines (e), straight horizontal spines (g) and recurving spines (f). The oddest looking of these are perhaps those with straight horizontal spines and a triangular shield [19]. Among the peltate forms with crescent-shaped spines two groups become again quite distinct, namely those in which the spines continue to grow and to protrude as needlelike points beyond the wings (as in line d, 16) and those in which the growth of the wings overtakes that of the spines [24]. But not in all of the bicornis forms does the wing grow strongest at the base of the spines, in some it appears first in the middle of the spine as a small outgrowth (as in 5) and continues to grow strongest there and to taper towards both the base and point of the spine (as in 10 and 11). These individuals form a distinct group by themselves. By continued growth baglike wings are formed, like those represented in tier III [29 and 30; see also enlargements in text fig. 14, 15]. In this group which I have here designated as var. s i g n u m in allusion to the simi- larity of the extreme forms to the standards of Roman legions an inde- pendent outgrowth of two semicircular wings, forming together a disk, is found. This formation is best shown in text figure 14. From its pres- ervation partly below and partly above the other wing it appears that this disk partly overlapped the other older one and had a slightly oblique position, though also growing from the lateral face of the rhabdosome. Plate A <0 3 -t— > OD T3 C oo s CD CD C2- 32 24 20 21 30 y S7 33 34 T T 31 sa 25 T 22 35 2? r 2i Y 23 17 t g 38 3^ 37 15 \