Res oes Stine ‘es Ti 6 a ke « Spa rey clare eta yah fGE icaee 3 ‘a aimee har gt One e Be: en sarang entree ure ee rye Hoe pe oH he es ad 4 Sere easiness oo eee erry OH hi yt Sn, AS cate, Ug net i; ra ee a See Ps a 5 Bea e j Bie “See % ¥ api area enon fff Be sage PP Mig ign Se if J oe ty Me a sheer all gr a Sa rh ote oe a coo Sect fagoiine “litea, ED: 1 LF BLL, Shes arg reat a ete an Sony Papa 4 oii N Y fa : fens “ees a entre Say, th, Ba og Fe Aes i, HEV See : if a etacrtay 2 a ae Rear 4 | a Soe} Pai Site *semmesroes FR nqn nb ons ate kan PAR ts at ae aes em) “EB ay nat Reape Sn 8 : ae fei EE eG Ae EP Pee ee tain Fy a Pt AEE : wat Paget, La Vitecnonee” sue a pO a Fitba ae ate pyayeee Ml a eet Ee ee 3 ‘i a Ay ati ii tnt © Hi iM | be be : has , | oe = | ’ aw % Nest Ay SA ve Asay, ~/ OF THE er N.C NUN ACE T MOGTETY OF NATURAL WIMOnY. PUBLISHING COMMITTEE: S. A. MILLER, _F. W. LANGDON, Cc. F. LOW, Jj. KF. JUDGE. > GEO. W. HARPER. WOlL, IV 16st. CINCINNATI: PRINTED BY JAMES BARCLAY, 269 VINE STREET. t INDEX -TO_VOL. TY. PAGE. PLCTIMGCKINUS COPEL....0.....ccsscoee cceceeree 310 Actinocrinus dalyanusS..........cccceseeees 309 Pe NSATICOCLINUS CLASSUS.......0. ..sceseoeccees 178 PISUPICOCKINUS CLESANS. .........c8eesencanes 179 PR MUP FCR MS IFASTIIG.....00..000e5sseoneqen saaves 308 Amygdalocystites huntingtoni ......... 177 American Association for the Ad- vancement of Science.............. 179 Anthropological notes, by F. W. HOMO 3 co hake tre ese deeb 'ewsevenie 237. Athyris lamellosa ...... (ee Bn A ey 307 Athyris planosuleata...........cce.csbZore 307 Books received by donation, ex- change and purchase............... 347 Cenozoic age or Tertiary period continued, by S. A. Milter... 3- Cenozoic age or Tertiary period continued, by S. A. Miller...93- 144 Cenozoic age or Tertiary period continued, by 8S. A. Miller 183- Camarophoria occidentalis............... Century plant, by Joseph F. James... Chambers, V.T., Two new species of 46 INVOTMOSELACH.siin.s00c00s 000 ccacanoates 47 Wolpowends Clark €livs....s..cccseerss coecapene 77 Colvin, Prof. Wm., Notice of his life UMNO ESET VA CES: caiscnaasesentaces occuccess 265 Conchology—Zvological miscellany .. 345 Cumeamiy Cliptica......0.6.isvcecceceeces 317 ROME MOCTAMUS COLD va... .0ecsecneveersteees ons 174 Cyathocrinus vanhorneéi...............048 261 Cyathophyllum subcespitosum ........ 308 Cyclocystoides magnus ..............006 70 Cyrtoceras conoidale ..............606.0008. 78 CyrtOCeras ITVESUlATE.........06.0.e.ceeseee 79 PUR ISUMMC AM ay, tac hecsesesahs yaisnae Setieeceecdee cays LUCEY Dendrocrinus erraticus ............66..00 316 Description of some new and re- markable crinoids and other fossils of the Hudson River Group, and notice of Stroto- crinus bloomfieldensis, by’. A. Miller Description of new fossils from the Lower Silurian and Subear- boniferous rocks of Ohio and Kentucky, by A. G. Wetherby Descriptions of new fossils from the Lower Silurian and Subearbon- iferous rocks of Kentucky, by PMCID VVCLITCL DY! chevcevos ser satnbadee Description of a new species of Patula, and remarks upon a Hyalina, by Geo. W. Harper ... Description of new species of fossils, PASE CAC MGT ten eciccd ae wes eacoee Description of new species of fossils from the Hudson River Group, Oe er ry 69 Cb e and remarks upon others, by SpA MRC r rh! c0s vccusscs juvescass 316 Diaptomus kentuckyensis ............... 48 PAGE. Doryerinus Limeatus.: As. -0.- <6 secant 310 Dury, Charles, Description of the young of the grizzly bear-Ursus jae etl eS GS Re anne ere ROPMAT GSPEIG ae once 68 Entomology, in Zoological miscellany 34 Entomostraca, two new species, by V. MAIC AIM hse oc. 05. sess eer nen 47 Field notes on Louisiana birds, by Ba We an ed ony e PAGE. PAGE. monuments of Anderson town- Proetus granulatus _...c:53 saeeepeaeeeeee 81 ship, Hamilton county, Ohio... 293 | Proetus peroccidens ..........06sseeee sence 308 Miller, S. A., Th- Cenozoic age or PyanOMya © ....4.\...00. ses anes 318 Tertiary period continued ...3— 46 | Pyanomya gibbosa.........ssssessessesseepes 318 The Cenozoic age or Tertiary period continued .......c...-ces-« 93-144 The Cenozoic age or Tertiary period continued—the drift of the Central part of the Con- tinent—completing the Meso- zoic and Cenozoic Geology 183-234 Description of some new and remarkable Crinoids and other fossils of the Hudson River Group, and notice of Stroto- crinus bloomfieldensis............ New species of fossils and re: marks upon others from the Niagara Group of Illinois........ Description of new species of fossils Observations on the Unification of Geological Nomenclature, with reference to the Silurian formation of North America... Subcarboniferous fossils from the Lake Valley Mining Dis- trict of New Mexico, with de- se’ iption of new species Description of new species of fossils from the Hudson River Group, and remarks upon OLMOMSS fe. capone tcekenns Seer ene Op lege New species of fossils, and remarks upon others from the Niagara Group of [llinois, by S. A. Miller Observations on the Unification of Geological Nomenclature, with special reference to the Siluri- 69 166 259 Ce eee scoeesessessresoes cesesesess sseres 306 see reoee2 Pewee eee e eae tet ses scores cesses sesees an formation of North America, Oe Sere a Gare WG IS ams Reyne ea ces 26 Officers of the Society. ......2sccsscvatesees 9 Ornithology in Zoological miscellany 337 MPa aS ANY AIA, 52s Love see selsninw ng ovis omer 313 OR Mesa HC IL CNIMT. © 5.0..0.j5c0%ehbe see nastar 307 OrmMis CESUPINALA 2.2.0. .ccooncebshae sectors 307 OTEROCeEras DYYNES1 ...c0.0s0sseeapvaneve. +0 319 Orthoceras cincinnatense ...........+ 319 OTE DBCETAS TOSUCT.,..... 57. .rcmaariecelnsess 319 Orthoceras Harper]... sec icseteeosaevesw cee 319 Orthodesnig, DYTUCSL......0:--seorestnars 76 Paleaster SKCMIPLUS 2.235056 .00ssccosensenns 69 Pet Gla nOe Yat fears ajc se ease aa mvebiet amass 258 Platyceras wquilaterale (1.5. ..2....--..2. 307 Platyerinus, oer laa. secon se meses ss 311 Prehistoric monuments of Anderson township, Hamilton county,O., by Charles die Meta. i... ccmssene' 293 Proceedings of the Society............... 1 Proceedings of the Society............... 91 Proceedings of the Society............... 181 Proceedings of the Society......... Ba a 263 Productus semireticulatus ............++ 307 PFOUECtUS VIWTATUS ...<.:.ch sontay sesnes ite rns 307 Quercus macrocarpa—Variability of the acorns, by Jos. F. James... 320 Report of the committee on the-life and character of Geo. Graham 85 Report of the committee on the life and services of Prof. Wm. Col- VTE ios das. chb sees yeh as niece ee 265 Report of the committee on Mrs. Abi- wail W AQnren. <2: 4.nisesenersineeerees 266 Weteocrinus Sracilis ..,......eesesseaeweeere 83 Rhynchonella pugtulosa ..........0..s0eee 307 Rhynchonella tuta.-..:25..01 sae eee 315 SAC COCKINMBS tins et +i. sneeeweteaian cayenne 167 SAC COGINMDUS CLANI .. aco. -sacaeennsreeeetee 173 Saceocrinus infelix .:..cscsssssesenee .... 260 SaccocrinUs MALPCOUANUS.........00 covers 167 SACCOCEINUS MEGCIS \.f)05-0.-s- cs veceene a As 172 Saccocrinus urniformis .......ccsecseeres 170 Some notes on American land shells, by A. G. Wetherby \icececns-e 323 Spirifera novamexXiCana ........seeeseeeee 314 Spirifera rockymontana .............e000 307 Spiti fers, Strtatas. :..5..ce .cevsse-paemeeeeee 307 Spirifera fem eravia >ss:..2...0.crcneqpepnees 314 Strophomena rhomboidalis............... 306 Strotocrinus bloomfieldensis ............ 76 Subecarboniferous fossils from the Lake Valley Mining District of New Mexico, with descrip- tion of new species by S. A. MiMM Gr 23. eicceeces 0 ese si hong 306 Daehidius fonticola. ......2:. snecsessaeeee 47 | Trematodiscus konincki..........06 esse. 79 Trematodiscus rockymontanus........ 312 Trematopora AMELICANA .........seceeeene 312 Triconia Steel: :++--)s-cs- aenseeeemeny 259 Ursus horribilis:...... vec. aesuseeheeeee 68 Variability of the acorns of Quercus macrocarpa, by Jos. F. James.. 320 Warren, Mrs. Abigail, Report of the committee in memory of......... 266 Wetherpy, A. G., Description of new fossils from the Lower Silurian and Subearboniferous rocks of Ohio and Kentucky .:............. a7 On the Geographical distribu- tion of certain fresh-water mol- lusks of North America, and the probable causes of their VAIN VAL OLS 4 bes techie ce > eee eee 156 Descriptions of new _ fossils from the Lower Silurian and Subearboniferous rocks of Kientuehoy. 2.00: !spn5 os cers sneer eaee 177 Some notes on American land SHGMIS Av ravees ss ceanuts deh o> a pee 323 KON OCTLAUS. 0k i 0 iets cnn bene .0 done pee vt Xenocrinus penicillus .......ceeesseeee 72, 171 Zoological miscellany, by F. W. Panedon .........00¢+se ikon waseRe eee 336 THE JOURNAL CNCANATH SCTRTY GR NATURAL HISTORY PROCEEDINGS OF THE SOCIETY. 7 Turspay Evernine, January 6, 1881. Dr. R. M. Byrnes, President, in the chair. Davis L. James, Secre- tary pro tem. Present, 12 members. Prof. F. W. Clarke was elected a member of the Society. Mr. W. M. Linney donated specimens of Péilodictya hilli, a copy of his report on the timbers of Boyle and Mercer counties, Kentucky, and a specimen of the wood of Cladrastis tinctoria, or yellow wood, a tree not uncommon in the Alleghanies, but rare in this locality. Turspay Evenine, February 1, 1881. Dr. R. M. Byrnes, President, in the chair, Present, 15 members. Dr. A. T. Keckeler, and A. V. Stewart, were elected members of the Society. L. S. Cotton made some remarks upon the meteorological observa- tions which have been made in this locality, and urged the importance of full and complete weather reports. A. E. Heighway, Jr., presented specimens of native copper, tremolite, actinolite, and slikensides, from the west; and Mr. J. E. Frey presented a fine specimen of the sea sturgeon, which is splendidly mounted by Mr. Shorten, hie SRS a, Cincinnatt Society of Natural History. bo Turspay Everntnc, March 1, 1881. Dr. R. M. Byrnes, President, in the chair. L. S. Cotton, Secretary pro tem. Present, 20 members. Joseph F. James read a paper on the geographical distribution of plants, etc., which is published elsewhere in this No. of the J OURNAL. Dr. A. ‘J. Howe exhibited a drawing (one tenth of the natural size) of the whale on exhibition in this city. He showed that it had been erroneously called the Greenland or Right whale, whereas it is the Balenoptera boops, or fin-whale, or rorqual of the Norwegians, a mam- mal not less interesting than the true Balena, though of much less value both for oil and baleen. He described its peculiarities in a very interesting address, that was warmly received by the members present. S. A. Miller made some remarks upon the glacial theory, taking the position that the so-called continental glacier and glacial period of this continent are purely the work of the imagination, andare not founded upon any of the known geological facts. He followed the views of Dawson respecting the Pliocene period, in the region of the Gulf of St. Lawrence, Lake Champlain, Hudson river, and the New England States, and showed that the drift of the central part of the Continent was not connected with the drift ofthe eastern part, and therefore not, necessarily, contemporaneous with it. He dwelt upon the absence of drift phenomena in the Rocky mountain region, and claimed that the castellated rocks of the Bad Lunds of the west, and the outliers of pinnacled sandstone, in Wisconsin and other parts of the country, are unimpeachable witnesses, bearing lasting testimony against the con- © tinental glacier and the so-called glacial period. Dr. O. D. Norton announced that Geo. Graham, a life member of the Society, had that evening departed this life, and on motion of Dr. A. J. Howe, a committee, consisting of Dr. A. J. Howe, Dr. O. D. Nor- ton, and U. P. James, was appointed to draft suitable expressions of the esteem in which he was held by the Society, and such remarks up- on his life and character as might seem desirable. On motion of V. T. Chambers, the committee were authorized to place their report in the hands of the publishing committee, for appearance in this number of the JourRNAL, without waiting to have it first read to the Society and entered on the journal. Prof. Mickleborough presented a Cephalopod from near Province- town, Massachusetts. vs ieee — 2 we Mesozoic and Cenozoic Geology and Paleontology. 5] THE CZANOZOIC AGH OR TERTIARY PERIOD. By S. A. Mituer, Esq. [Continued from Vol. wit., page 288. | In 1858, Dr. F. V. Hayden* prepared a vertical section, showing the order of superposition of the different beds of the Tertiary Basin of White and Niobrara rivers. The Miocene, he divided, in ascending order, as follows: 1. Bed A.—Light gray, fine sand, with more or less calcareous matter, passing down into an ash-colored plastic clay, with large quantities of quartz grains disseminated through it, sometimes form- ing aggregated masses like quartzose sandstone cemented with plaster; then an ash-colored clay with a greenish tinge, underlaid at base by a ' light gray and ferruginous silicious sand and gravel, with pinkish bands. Immense quantities of silex, in the form of seams, all through the beds. Titanotherium Bed. Found on Old Woman’s creek, and in many localities along the valley of the South Fork of Shyenne, Best development on Sage and Bear creeks. Seen at several localities in the valley of White river. ‘Thickness, 80 to 100 feet. 2. Bed B.—A deep flesh-colored, argillo-calcareous, indurated grit; the outside, when weathered, has the appearance of a plastic clay. Passes down into a gray clay, with layers of sandstone; underlaid by a flesh-colored, argillo-calcareous stratum, containing a profusion of Mammalian and Chelonian remains, Turtle and Oreodon Bed. Found on Old Woman’s creek, a fork of Sbhyenne river, on the head of the South Fork of the Shyenne; most conspicuous on Sage and Bear creeks, and at Ash Grove Spring, and well developed in numerous localities in the valley of White river. Thickness, 80 to 100 feet. 3. Bed C.—Very fine, yellow, calcareous sand, not differing very materially from Bed D, with numerous layers of concretions, and rarely organic remains, passing down into a variegated bed, consisting of alternate layers of dark brown clay, and light gray, calcareous grit, forming bands, of which twenty-seven were counted at one locality, from one inch to two feet in thickness. Found on White river, Bear creek, Ash Grove Spring and head of Shyenne river, but most con- spicuous near White river. Thickness, 50 to 80 feet. 4. Bed D.—A dull, reddish-brown, indurated grit, with many layers of silico-calcareous concretions, sometimes forming a heavy-bedded, * Proc. Acad. Nat. Sci., vol. x. 4 Cincinnati Society of Natural History. fine-grained sandstone, and containing comparatively few organic re- mains. Found on the Niobrara and Platte rivers; well developed in the region of Fort Laramie, and in the valley of White river; and con- Spicuous, and composing the main part of the dividing ridge between White and Niobrara rivers. Thickness, 350 to 400 feet. 0. Bed H.—Usually a coarse-grained sandstone, sometimes heavy | bedded and compact; sometimes loose and incoherent, and varying much indifferent localities. It forms immense masses of conglomerate, and contains layers of tabular limestone, with indistinct organic re- mains, and a few mammalian remains, in a fragmentary condition. It passes gradually into the bed below. It is most fully developed along the upper portion of Niobrara river, and in the region around Fort Laramie. It is seen also on White river, and on Grindstone hills. Thickness from 180 to 200 feet. The Pliocene consists of ist, dark gray or brown sand, loose, in- coherent, with remains of mastodon and elephant ; 2d, sand and gravel, incoherent; 3d, yellowish-white grit, with many calcareous, arenaceous concretions ; 4th, gray sand with a greenish tinge, which contains the greater part of the organic remains; Sth, deep yellowish-red arenaceous marl; 6th, yellowish-gray grit, sometimes quite calcareous, with numerous layers of concretionary limestone, from two to six inches in thickness, containing fresh water.and land shells, closely allied, and perhaps identical with living species, which belong to the genera, Succinea, Limnea, Paludina and Helix. It contains also, much wood of coniferous character. It covers a very large area on Loup Fork, from the mouth of North Branch to the source of Loup Fork, and occurs in the Platte valley. Itis most fully developed on the Niobrara river, and extends from the mouth of Turtle river three hundred miles up the Niobrara. It occurs on Bijou hills, and Medicine hills, and is thinly represented in the valley of White river. Thickness from 300 to 400 feet. A . The Post-pliocene consists of yellow, silicious marl, similar in its character to the loess of the Rhine, passing down into variegated indu- rated clays, and brown and yellow fine grits. It contains the remains of extinct quadrupeds, mingled with those identical with recent ones, and a few mollusca, mostly identical with recent species. It is most fully developed along the Missouri river, from the mouth of the Nio- brara to St. Joseph, and occurs in the Platte valley and on the Loup Fork. Thickness from 300 to 500 feet, ' Prof. G. C. Swallow* referred a formation made up of clays and * Proc. Am. Ass. Ad. Sci. — or Mesozoic and Cenozoic Geology and Paleontology. sands and sandstone, extending along the bluffs, and skirting the bottoms, from Commerce, in Scott county, Missouri, westward to Stoddard, and thence south to the chalk bluffs in Arkansas to the Tertiary age. His section shows a thickness of 214 feet, but no fossils were obtained. Prof. E. Emmons* described, from the Eocene of Craven county, North Carolina, Carcharodon ferox, Cidaris carolinensis, Echinolam- pus appendiculatus, Echinocyamus parvus; from near Newbern, Car- charodon triangularis, Trygon carolinensis; from Wilmington, Car- charodon crassidens, C. contortidens, Cidaris mitchelli, Gonioclypeus subangulatus, Lunulites oblonyus; and from other places, Hemipristis crenulatus. | He described, from the Miocene at Elizabethtown, and near Cape Fear river, Bladen county, North Carolina, Polyptychodon rugosus, Llliptonodon compressus, Fusus equalis, L’. lametlosus, &. monilifor- mis, Lasciolaria elegans, Ff. alternata, F. acuta, £. nodulosa, £. spar- rowt, Cancellaria carolinensis, Buccinum moniliforme, B. multilineat- um, Voluta obtusa, Paludina subglobasa; and from the marl of other places, Galeocerdo sub-crenatus, Pycnodus carolinensis, Terebra ne- glecta, Dolium octocostatum, Marginella constricta, M. elevata, Pleu- rotoma elegans, P. flecuosum, P. tuberculatum, Pyramidella reticu- lata, Chemnitzia reticulata, Hulima subulata, Cerithium annulatum, C. bicostatum, Terebellum constrictum, »calaria curta, Littorina line- ata, Delphinuia quadricostata, now Carinorbis quadricostatus, Torna- tina cylindrica, Cecum annulatum, Pecten princepoides, Chama stri- ata, and Artemis transversus. Prof. F. $. Holmes+ described, from the Post Pliocene of South Carolina, Nodosaria obtusa, Astrea crassa, Pectunculus charleston- ensis, Lucina kiawahensis, Tapes grus, Mulinia milesi, Mesodesma concentricum, Abra angulata, Mya simplex, Cavolina tuomeyi, Fusus conus, Ff’. filiformis, f&. bullata, &. rudis, Volutomitra wandoersis, Turbonilla cancellata, T. quinquestriata, T. lineata, T. subulata, T. caroliniana, T. acicula, T. subcoronata, Obeliscus crenulatus, Archi- tectonica gemma, Angaria crassa, and Adeorbis nautiliformis. Dr. B. F. Shumard{ described, from rocks supposed to be of Eocene age, at Port Orford and at Davis’ Coal Mine in Oregon Territory, Zu- cina fibrosa, Corbula evansana, Leda oregona, now Nuculana ore- * Geo. Sur. N. Carolina, * + Post Pliocene Fossils of South Carolina. t Trans. .St. Louis Acad. Sci., vol. i. 6 Cincinnat, Society of Natural History. gona, L. willamettensis, now N. willamettensis; and from gray, fine- grained sandstone, at the mouth of Coose Bay, Pecten coosensis, and Venus securis. . Dr. Leidy* described, from the Pliocene of the Niobrara river, Ne- braska, Mastodon mirificus, Procamelus gracilis, P. robustus, P. occt- dentalis, Canis haydeni, C. sevus, C. temerarius, C. vafer, Felis in- trepidus, now Pseudelurus intrepidus, Aelurodon ferox, Hystrix ven- ustus, Castor tortus, Cervus warreni, Megalomerys niobrarensis, Mery- chyus elegans, M. major, M. medius, Hypohippus afinis, Parahippus cognatus, Equus excelsus, EL. fraternus, Protohippus perditus, Mery- chippus mirabilis, Rhinoceros crassus, Euelephas imperator, and from the red grit bed of Niobrara, near Fort Laramie (Miocene), Meryco- choerus proprius. In 1859, James Richardsont made a geological exane ane of the Gaspe peninsula, and observed two terraces in the drift tu the west of Trois Pistoles river, at 130 and 300 feet, respectively, above the sea, and another at the mouth of the Matanne. at the height of 50 feet. Stratified clay occurs at the head of lake Matapedia, 480 feet above the sea and near the outlet at the height of about 530 feet. Marine testacea occur in the terrace on the east side of the Matanne river at the height of 50 feet above the sea; about two miles west of the Metis river, at the height of 130 feet, and eight miles up the Metis river, at 245 feet above the sea. At the St. Anne river there are five or six terraces in a height of 25 feet, abounding in fragments of marine shells. Grooves and scratches were observed a half mile below Trois Pistoles church, 60 feet above the sea, bearing 8S. 32 deg. E., and on the Kempt road, two miles from Lake ee age 630 feet above the sea, and bearing 8S. 80 deg. E. W. E. Logant explored the river Rouge, a branch of the Ottawa, to the Iroquois Chute: about fifty miles from the mouth. He found an undisturbed deposit of clay on the left bank of the river, on the fourth range of Grenville, 280 feet above Lake St. Peter. In the rear of Gren- ville and front of Harrington, not far east of the Rouge, there spreads out a flat surface of several hundred acres in extent, which is under- laid by clay, and has a height of about 000 feet above Lake St. Peter. The plain of the three mountains has an elevation above the ordinary summer level of the river, of about 30 feet, and above Lake St. Peter of * Proc. Acad. Nat. Sci., vol. x. 7 Rep. of Progr. Geo. Sur. of Canada. { Geo. Sur. of Canada, Rep. of Progress. Mesozoic and Cenozoic Geology and Paleontology. 7 about 585 feet. It consists, in general, of sand or fine gravel at the top, with clay interstratified toward the lower part, but the sand greatly predominates. The surface of the rocks in the valley wherever ex- amined were found to be grooved and striated. The courses of the grooves vary from S. 30 deg. E, to 8. 25 deg. W., and accord in a gen- eral way, with the direction of the valley. The limits of the valley evidently guided the direction of the moving masses which produced the strie, Prof. Leo Lesquereux* described, from the Pliocene near Sommer- ville, Fayette county, Tennessee, Salix densinervis, Quercus saffordi, Andromeda dubia, and Eleagnus inequalis. In 1860, Prof. E. W. Hilgard}+ divided the Tertiary of Mississippi in ascending order into, Ist, The Northern Lignitic Group; 2d, The Claiborne Group; 3d, The Jackson Group; 4th, the Vicksburg Group; dth, The Grand Gulf Group. The Northern Lignitic Group occupies the central part of Northern Mississippi, and though generally covered by later deposits it out- crops at numerous places and is found at alldeep borings. It consists of estuary deposits of sandstone, with marine shells; gray clays and sands, and dark brown .and yellow clays and sands with lignite. Kstimated thickness, including the Claiborne Group, 425 feet. _ The Claiborne Group is found in the central part of the northern half of the State, in Holmes, Atala, Carroll and Choctaw counties, and in the western part of the State in Clarke, Lauderdale, Newton and Scott counties. It consists of blue and white marls, the latter always sandy and often indurate, and sandstones and claystones with some- times lignitic clays and sands. The Jackson Group forms a band across the central part of the State through Wayne, Clarke, Jasper, Newton, Scott, Madison and Yazoo counties. It consists of white (often indurate) and blue marls, highly fossiliferous. Estimated thickness, 80 feet. | The Vicksburg Group is the highest of the marine Kocene, and the only one which reaches the Mississippi river. It occupies a narrow _ belt of nearly uniform width, south of the Jackson Group, and extend- ing across the State from Vicksburg to the Alabama line, and thence to the Tombigbee river, where it forms the bluff at St. Stephens. It consists of crystalline limestones and blue marls with ferruginous strata. It is the only one of the marine stages of the Eocene which * Am. Jour. Sci. & Arts, 2d ser., vol. xxvii. + Geo. of Miss. , 8 Cincinnati Society of Natural History. exhibits crystalline limestones. It is highly fossiliferous. Estimated thickness, including the lignite at its base, 112 feet. The Grand Gulf Group covers an immense extent of country south of the Vicksburg Group, and is composed essentially of clays and sandstones, the latter generally rather aluminous and soft, and of ‘white-gray and yellowish-gray tints; the sand being very sharp. It - takes its name from the bluff at Grand Gulf on the Mississippi river, where it is well exposed. It is overlaid near the coast by strata of Pliocene and Post-pliocene age. Estimated thickness, 150 feet. Prof. F. 8S. Holmes* made three vertical sections of the Post- phogete strata of South Carolina in descending order as follows: - 1. The marine bed of the Wadmalur, consisting of yellow sand, 15 feet; ferruginous sand with casts of shells, 2 feet; red clay, 2 feet; and gray sand and mud with comminuted shells and fossils in fine preser- vation, 34 feet. , 2. The Ashley river beds, consisting of yellow sands with bands of ferruginous clay, 4 feet, and blue mud resting on the white Hocene marl, 1 foot. 3. The Goose creek beds, consisting of yellow sand, 12 feet; blue mud, 2 feet; ferruginous sand containing bones, 3 inches; yellow sand, 3 feet; and Pliocene marl resting on the Eocene white marl, 12 feet. The fossil bones obtained from these strata are often in a fine state of preservation, especially those taken from the blue mud, which are generally petrified; those from the sands are likewise well preserved, but in the peaty or upper beds they are not so petrified, retain all their gelatin and appear to decompose rapidiy. ‘They consist of the bones _ of horses, hogs, dogs, rabbits, beavers, the tapir, and other mammalian remains. T, A. Conradt Teves tesuk from the Eocene of Alabama and Missis- sippi, Hailia pergracilis, Volutilithes limopsis, V. rugatus, Athleta leioderma, Simpulum showwalteri, S. autopsis, S. exilis, Galeodia tri- carinata, Cithara nereidis, Murex morulus, Pseudoliva tuberculifera, Scala lintea, S. octolineata, S. staminea, Acteonina subvaricata, - Tornatellea bella, Cerithioderma prima, Mazzalina pyrula, Leda. bella, DOW Nuculana bella, L. eborea, now N. eborea, Axinea belli- sculpta, Diplodonta astartiformis, D, deltoidea, Crenella latifrons; from Texas, Pseudoliva carinata, P. fusiformis, P. linosa, Piper spectiva, and Monoptygma crassiplica. * Proc. Acad. Nat. Sci., vol. ii., and in Post-pliocene Foss. S. Carolina. + Jour. Acad. Nat. Sci., 2d ser., vol. iv. Mesozoic and Cenozoic Geology and Paleontology. 9 Wm. M. Gabb described, from the Eocene at Wheelock, and in Cald- well county, Texas, Belosepia ungula, Odontopolys compsorhytis, Fusus mortontopsts, Neptunea enterogramma, Turris mooret, T. kel- loggi, now Surcula kelloggi, T. nodocarinata, now Surcula nodocari- nata, T.retifera, T. texana, Hucheilodon reticulatum, Scobinella crassi- plicata, S. leviplicata, Distortio septemdentata, Phos texanus, Agaro- nia punctulifera, now Olivula punctulifera, Fasciolaria polita, F. mooret, now Cordiera moorei, Cymbiola texana, Mitra exilis, M. mooreana, now Lapparia mooreana, Hrato semenoides, now Mar- ginella semenoides, Neverita arata, Lunatia mooret, Architectonica meekana, A. texana, A. vespertina, Spirorbis leptostoma, Turritella nasuta, Hulima exilis, FE. tenua, Dentalium minutistriatum, Ditrupa subcoarctata, now Gadus subcoarctatus, Bulla kelloggi, Volvula conradana, V. minutissima, Helcion leanus, Corbula texana, Tellina mooreana, Leda compsa, now Nuculana compsa, Noetia pulchra, Crassatella antestriata, Anomia aphippioides, Serpula texana; from Alabama, Cirsotrema megaptera, Leiorhinus crassilabris, Axinea intercostata, and Pecten spillmani, He described, from the Miocene, near Shiloh, New Jersey, Cantharus cumberlandana, Fasciolaria woodi, Natica hemicrypta, Mercenaria cancellata, and from Maurice river, New Jersey, Ostrea mauricensts. Gabb and Horn described, from the Eocene, in Caidwell county, Texas, Flabellum pachyphyllum and Trochosmilia mortont. Prof. Leo Lesquereux* described, from the lower Eocene or lgnitic Tertiary of Tennessee and Mississippi, Magnolia hilgardana and Rhamnus marginatus. Meek and Haydent described, from the Miovene of the Bad Lands of White river, Planorbis letdyi and P. vetulus. Prof. J. W. Dawson described, from the Pliocene of Labrador, the foraminifer, Nonionina labradorica. In 1861, Prof. C. H. Hitchcock§ said that there is not a mountain in Maine, fragments of which will not be found scattered over the coun- try to the south or southeast. The granite of the Katahdin region is scattered over the southern part of Penobscot county, and the rocks of Mt. Abraham and Mt, Blue may be recognized among the bowldersi n Kennebec county. One of the effects of the drift action is the smooth- * Geo. of Ark., vol. ii. t Proc. Acad. Nat. Sci. C n. Nat. and Geo., vol. v. 2 Rep. Geo. Maine. Oa Cincinnati Society of Natural History. ing, rounding, scratching and furrowing of the ledges over, which the drift materials have passed, and unless these ledges have been decom- posed upon their surfaces, they are covered with scratches or striz, usually parallel to one another, and indicating the course of the drift agency. Ledges of talcose and argillaceous rocks preserve these mark- ings the most distinctly. Were the rocks of Maine laid bare, fully half - the surface would show these marks of smoothing. The course of the striz ‘in Maine vary from north 70 deg. west to north 80 deg. east. : At the Lubec lead mines, a series of striz were observed upon the side of a perpendicular wall, following the course of the wall around a corner. The course of the striz ultimately varied at right angles from their original directions. At several places at the sea shore the striz have been noticed below high water mark, and others were seen to run under the ocean at low-water mark. The course of the strize upon the lakes north of the Katahdin mountains have more of an easterly course than those to the east and south of the same mountains. It locks as if the mountains formed an obstruction around which the striating agency operated, in preference to climbing the elevation. It is a curious fact, in the same connection, that the stris are wanting on the sum- mit of Katahdin. It appears also that there was another deflection of the course of the strize in the valley of Sandy river. Mt. Abraham may have arrested the drift current on the north and turned it into Sandy river valley on the west, from which deflection it struck against the Saddleback mountain range, continued to Mount Blue, and was then directed toward French’s Mountain in Farmington. Drift strize are never found upon the south side of mountains, unless for a short distance, where the slope is very small. It is common to see different courses of strize intersecting one another, as on the south side of Chamberlin lake, where striz north 70 deg. west and north 50 deg. west intersect, and north 17 deg. west and north 67 deg. west in- tersect. | The only examples of glacial markings discovered, in Maine, are on the St. John river, in its upper portion. Above the Lake of the Seven Islands, on this river, there are no glacial markings, unless the scratches upon the pavement of bowlders are to be referred to them. The bed of the river is full of stones, and upon the banks below high- water mark they are as firmly set as paving stones in the streets of a city. The scratches are not as constant and distinct as those of the glacier below, and may possibly have been formed by ice freshets in Mesozoic and Cenozoic Geology and Paleontology. ED the spring of the year. Descending the river to No. 14 we find a ledge which has been struck by a force descending the river, as the stoss and lee sides plainly show. The course of the strie is north 65 deg* west, _the stoss side being on the southeast. A similar example occurs near the mouth of Black river, where the course of the striz is toward north 60 deg. west. The country above Black river being quite level, is not so well adapted for the existence of a glacier as the region below, where high mountains crowd the river on both sides. At the mouth of Little Black river the upper side of the ledges is uniformly the struck side. Some of the ledges are covered with both drift and glacial strive, the former coming from north 60 deg. west, and the latter running down the river northeasterly. A mile above the mouth of the St. Francis river, the glacial strize run down the river with the direction north 47 deg. east. Near the village of St. Francis the two sets of striz appear again, the drift with the di- rections of north 60 deg. west, and north 20 deg. west, and the glacial with the direction of north 16 deg. east. This is the course of the river around a curve. The former are here the most prominent,. In the township below Fort Kent, striz appear running north 30 deg. west. One of the finest exposures of the glacial striz is in Dionne, where the river makes a great bend and pursues a northerly course. The strize change with the river and run north 20 deg. west. or directly cpposite to the normal course of the drift in the vicinity, the force having gone northerly instead of southerly. No glacial markings were observed be- low this, in fact the glacial and drift markings could not be distin- guished from each other below the Madawaska settlements. The evi- dence for an ancient glacier is not so strong on the St. John river as in the western part of New England. Some might contend that the immense ice freshets in the spring would be sufficient. to explain all the phenomena. On the other hand, the objection to glaciers in north- ern Maine would be less than in Massachusetts, on account of the colder climate. An unstratified mass of a stiff, dark, bluish clay, containing rounded and striated bowlders, and called bowlder clay, is found on the precip- itous banks of rapid streams in narrow valleys. It underlies the finer sands and gravels of later periods, and always rests directly upon the solid rocks. | Modified drift occurs, in Maine, in the form of moraine terraces, horsebacks, sea beaches, sea bottoms, marine clays and terraces. Mo- raine terraces are generally accumulations of gravel, bowlders and sand, ; 3 4 > : 12 Cincinnatc Society of Natural History. often arranged in heaps and hollows, or conical and irregular eleva- tions with corresponding depressions. Mesozoic and Cenozoic Geology and Paleontology. 19 sandstones, without any appearance of eruptive rock, and also with very little metamorphism. . The unaltered sandstones extending along the Gavilian Range, near the San Juan valley, and forming the San Juan hills, which extend to the Pajaro river, are referred to the Miocene. In these hills the strata are very heavy bedded, and have a dip everywhere to the south. The materials of which they are made up are often coarse, and sometimes large enough to form a conglomerate, among the pebbles of which jas- per and other metamorphic rocks predominate. In the vicinity of the Bay of Monterey the granite is flanked by Mi- ocene sandstone. Both rocks are considerably altered, for a distance of about 20 feet from the junction; the sandstone is softened and dis- integrated, and the granite discolored. The metamorphism has so af- fected both rocks that it is not easy to determine the exact line of junction. The Miocene sandstones are displayed in some places in the region between the Canada de las Uvas and Soledad Pass, nearly 2,500 feet in-thickness, From the summit of the higher upturned strata, a wide belt of Tertiary rocks may be seen skirting the Coast Ranges, and worn into rounded hills, which are generally barren, especially on the west side of the Tulare valley. The Pliocene beds between Merced Lake and Mussel Point, on the peninsula of San Francisco, are made up of a bluish sandstone, of which the grains are cemented by carbonate of lime, interstratified with hard, fine conglomerates, of which the pebbles are evidently derived - from the adjacent jaspery rocks of Cretaceous uge. These strata con- tain Scutella interlineata, Crepidula princeps, both of which are ex- tinct, together with several species still living on the coast. At the head of Pleasant valley, the strata are overlaid by beds of volcanic ashes, interstratified with gravels, the whole series being con- formable and dipping at a low angle tothe east. They appear to be of Pliocene age, and identical in most respects with the sedimentary vol- canic beds to the north of Kirker’s Pass. To the north of San Pablo are low hills of very recent strata, which are nearly horizontal, and which rest unconformably on the edges of the Tertiary. They are referred to Post-pliocene age. From Tres Pinos, 13 miles from San Juan, to Booker’s, a distance of about 13 miles in a direct line, the road follows the Arroyo Joaquim Soto, a branch of the San Benito. Along this road there are vast de- posits of gravel, or entirely unconsolidated detritus, and which form a 0 Cincinnat. Society of Natural History. large portion of the series of ridges between’ the Gavilan, on the one side, and the Monte Diablo Range on the other. At the first exposure, about two miles beyond Tres Pinos, the stratified detritus forms a steep bluff about 400 feet above the creek. The gravel is made up of pebbles of granite, red and green jaspers, and silicious slate and other metamorphic materials. At a point a tew miles below Bookers the strata are worn into precipitous canons, with bare bluff banks or al- most perpendicular walls, regularly stratified, and varying in fineness from a coarse gravel to fine sand, with here and there a thin band of - consolidated materials, the remainder entirely in the original condition in which it was deposited, as far as being held together by any cement is concerned. The thickness of these deposits is enormous; one hill was found to be 1,274 feet above the valley, and another 1,800 feet. Both these hills are entirely made up of these unconsolidated materials. This region gives one a most vivid idea of how recently geological changes of magnitude have taken place in this part of the State, and furnishes most impressive testimony to add to that obtained in other places, in relation to the lateness of the geological epoch, during which this portion of the chain was elevated. It would appear that the basin, in which these strata were deposited, was drained of the water at suc— cessive intervals, by the elevation of the basin itself, judging from the disturbed position of the strata it contains, and not by the gradual wearing away of a barrier at its lower end. Prof. J. W. Dawson* described the Post-pliocene deposits in the country around Cacouna and Riviere-du-Loup. The depressions be- ‘tween the ridges are occupied by these deposits resting upon the Quebec Group of rocks. The oldest member of the deposit, isa tough marine bowlder clay, its cement formed of gray or reddish mud, de- rived from the waste of the shales of the Quebec Group, and the stones ° and bowlders with which it is filled, partly derived from the harder members of that Group, and partly from the Laurentian hills, on the opposite or northern side of the river, more than twenty miles distant. The thickness of the bowlder clay is variable, but at Ile Verte, it forms - a terrace 50 feet in height. The bowider clay at Cacouna, is a deep- water deposit. Its most abundant shells are Leda truncata, Nucula tenuis, and Tellina proxima, and these are imbedded in the clay with the valves closed, and in as perfect condition as if the animals still in- habited them. The bowlder clay is also fossiliferous at Murray bay, St. Nicholas, and Cape Elizabeth. * Can. Nat. and Geol. new ser., vol. ii. Mesozoic and Cenozoic Geology and Paleontology. 21 Above the bowlder clay, there occurs a dark gray, soft, sandy clay, containing numerous bowlders, and above this several feet of stratified sandy clay without bowlders ; while on the sides of the ridges, and at some places near the present shore, there are beds and terraces of sand and gravel constituting old shingle beaches, apparently much more re- cent than the other deposits. All of the deposits are more or less fossiliferous. The surface of the rocks beneath the bowlder clay, is polished and striated in the direction of northeast and southwest, or that of the St. Lawrence valley. W. M. Gabb* described, from the Post-pliocene of San Pedro and Santa Barbara, Turcica coffea, and Calliostoma tricolor, Dr. Joseph Leidy+ described, from the Miocene of White river, Nebraska, Ahinoceros occidentalis ; from Texas, &. meridianus ; from Calaveras county, California, R. hesperius. And from the Pliocene of California, Hqwus occidentalis. R. P. Whitfieldt described, from the Eocene of the Southern States, Pisania claibornensis, Pyrula juvenis, Fulgur triserialis, Fusus tortilis, Pseudoliva elliptica, Monoptygma leat, Coluinbella turricula, Pleuro- toma capax, P. nasutum, P. persa, P. adeona, Voluta newcombana, Mitra haleana, M. biconica, Natica erecta, now Lacunaria erecta, N. perspecta, N. reversu, N. onusta, N. alabamensis, now Lacunaria- alabamensis, N. aperta, Velutina expansa, Cerithium vinctum, Po- tamides alabamensis, Turritella eurynome, T. multilra, T. alabamen- sis, Cucullea macrodonta, Crassatella tumidula. T. A. Conrad§ described, from the Jackson Group, at Enterprise, Mississippi, Corbula jfilosa, Dione securiformis, D. annexa, Tellina eburneopsis, T. albaria, T. linifera, Alveinus minutus, Spherella bulla, Cyclas curta, Protocardia lima, Gouldia pygmea, Axinewu in- equistriata, A. duplistriata, Nuculana linifera, Nucula spheniopsis, Arcoperna filosa, Pecten scintellatus, now Camptonectes scintellatus, Doliopsis quinquecosta, now Galeodia quinquecosta, Turritella perdita, Mesalia arenicola. From divers places in Alabama, Mississippi and Texas, Strepsidura lintea, Surcula gabbi, S. lintea, Cochlespira engonata, Moniliopsis elaborata, Drillia texana, Tortoliva texana, Monoptygma curta, Volutilithes indenta, V.impressa, Obeliscus perexilis, Architectonica * Pro. Cal. Acad. Sci. + Pro. Acad. Nat. Sci. t Am. Jour. Conch., vol. i. § Am. Jour. Conch., vol.i. . 22 Cincinnati Society of Natural History. celatura, Cancellaria impressa, C. tortiplica, Tornatellea lata,Corbula jilosa, Egeria donacea, Cytheriopsis hydana, Oyclas claibornensis, Mysia deltoidea, Conus alveatus, C. subsauridens, Cochlespira bella, Buccitriton altum, Limatia marylandica, Cirsostrema clatbornensis, Cancellaria ellapsa, Dentalium densatum ; from Shark river, Mon- mouth county, New Jersey, Pleurotomaria perlata, Surcula annosa, Acteonema prisca, and Avicula annosa. In 1866, Prof. J. W. Dawson* said the snow-clad hills of Green- land send down to the sea great glaciers, which in the bays and fiords of that inhospitable region, form, at their extremities, huge cliffs of ever- lasting ice, and annually ‘‘calve,”’ as the seamen say, or give off a great progeny of ice islands, which slowly drifted to the southward by the Arctic current, pass along the American coast, diffusing a cold and bleak atmosphere, until they melt in the warm waters of the Gulf stream. Many of these bergs enter the straits of Belle-Isle, for the. Arctic current clings closely to the coast, and a part of it seems to be deflected into the Gulf of St. Lawrence through this passage, carrying with it many large bergs. Mr. Vaughan, late superintendent of the light house at Belle-Isle, has kept a register of icebergs for several years. He states that for ten which enter the straits, fifty drift to the southward, and that most of those which enter pass inward on the north side of the island, drift toward the western end of the straits and then pass out on the south of the island, so that the straits seem to be merely a sort of eddy in the course of the bergs. The number in the straits varies much in different seasons of the year. The greatest number are seen in spring, especially in May and June; and toward autumn and in the winter very few remain. Those which remain until autumn are reduced to mere skeletons; but if they survive until winter, they again grow in dimensions, owing tu the accumulations upon them of snow and new ice. Those that we saw early in July were large and massive in their proportions. ‘The few that remained when we returned in September, were smaller in sizé, and cut into fantastic and toppling pinnacles. Vaughan records that on the 30th of May, 1858, he counted in the straits of Belle-Isle 496 bergs, the least of them 60 feet in height, some of them half a mile long and 200 feet high. Only % of the vol- ume of floating ice appears above water, and many of these great bergs may thus touch the ground in a depth of 30 fathoms or more, so that if we imagine 400 of them moving up and down under the influence of * Can. Nat. & Geol., 2d series, vol. ili- eel Mesozoic and Cenozoic Geoiogy and Paleontology. 23 the current, oscillating slowly with the motion of the sea, and grind- ing on the rocks and stone-covered bottom, at all depths, from the cen- ter of the channel, we may form some conception of the effects of these huge polishers of the sea floor. Of the bergs which pass outside of the straits, many ground on the banks off Belle-Isle. Vaughan has seen a hundred large bergs aground at one time on the banks, and they ground on various parts of the banks of Newfoundland, and all along the coast of that island. As they are borne by the deep seated cold current, and are scarcely at all affected by the wind, they move somewhat uniformly, in a direction from N, E. to 8. W., and when they touch the bottom the striation or grooving which they produce must be in that direction. In passing through the straits in July, we saw a great number of bergs, some were low and flat topped with perpendicular sides, others were concave or roof-shaped like great tents pitched on the sea ; others were rounded in outline or rose into towers and pinnacles. Most of them were of a pure dead white, like loaf sugar, shaded with pale bluish green in the great rents and recent fractures. One of them seemed as if it had grounded and then overturned, presenting a flat and scored surface covered with sand and earthy matter. After describing the glaciers of Mont Blanc, he lays down the following rules : 1. Glaciers heap up their debris in abrupt ridges. Floating ice sometimes does this, but more usually spreads its load in a more or less uniform sheet. | 2. The material of moraines is all local, icebergs carry their de- posits often to great distances from their sources. 3. The stones carried by glaciers are mostly angular, except where they have been acted on by torrents. Those moved by floating ice are more often rounded, being acted on by the waves and by the abrading action of sand drifted by currents. 4. In the marine glacial deposits, mud is mixed with stones and bowlders. In the case of land glaciers, most of this mud is carried off by streams, and deposited elsewhere. 5. The deposits from floating ice may contain marine shells. These of glaciers can not, except where, as in Greenland and Spitzbergen, glaciers push their moraines out into the sea. 6. It is the nature of glaciers to flow in the deepest ravines they can find, and such ravines drain the ice of extensive areas of mountain land. Icebergs, on the contrary, act with greatest ease on flat sur- faces, or slight elevations in the seat bottom. 24 Cincinnati Society of Natural History. 7. Glaciers must descend slopes, and must be backed by large sup- plies of perennial snow. Icebergs act independently, and being water- borne, may work up slopes and on level surfaces. 8. Glaciers striate the sides and bottoms of their ravines very un- equally,’acting with great force and effect only on those places where their weight impinges most heavily. Icebergs, on the contrary, being carried by constant currents, and over comparatively flat surfaces, must striate and grind more regularly over large areas, and with less reference to local inequalities of surface. 9. The direction of the striz and grooves produced by glaciers de- pends on the direction of the valleys, That of icebergs, on the con- trary, depends upon the direction of marine currents, which is not determined by the outline of surface, but is influenced by the large and wide depressions of the sea bottom. 10. When subsidence of the land is in progress, Py Es ice may carry bowlders from lower to higher levels. Glaciers can not do this under any circumstances, though in their progress they may leave blocks perched on the tops of peaks and ridges. He further said, that, in all these points of difference, the bowlder clay and drift of Canada, and other parts of North America, cor— respond rather with the action of floating ice than of land ice. More especially is this the case in the character of the striated sur- faces, the bedded distribution of the deposits, the transport of mate- rial up the natural slope, the presence of marine shells, and the mechanical and chemical character of the bowlder clay. He also enumerated the following Post-pliocene plants as occur- ring, in nodules, at Green’s Creek, and other places in Canada, to-wit: Drosera rotundifolia, Acer spicatum, Potentilla canadensis, Gaylus- saccia resinosa, Populus balsamifera, Thuja occidentalis, Potamo- geton perfoliatus, P. pusillus, Equisetum scirpoides. None of the plants are properly Arctic in their distribution, and the assemblage may be characterized as a selection from the present Canadian flora of some of the more hardy species having the most northern range. At Green’s Creek (near Ottawa) the plant-bearing nodules occur in the lower part of the Leda clay, which contains a few bowlders, and is apparently, in places, overlaid by large bowlders, while no distinct bowlder clay underlies it. The circumstances which accumulated the thick bed of bowlder clay near Montreal, were probably absent in the Ottawa valley. In any case, we must regard the deposits of Green’s Creek as coeval with the Leda clay of Montreal, and with the period Mesozoic and Cenozoic Geology and Paleontology. 25 of the greatest abundance of Leda truncata, the most exclusively Arctic shell of these deposits. In other words, he regarded the plants above mentioned as probably belonging to the period of greatest re- frigeration of which we have any evidence—of course, not including that mythical period of universal incasement in ice, of which, in so far as Canada is concerned, there is no evidence whatever. The Tertiary formation * exists in the southern part of the State of Illinois. It is best developed in Pulaski and Massac counties. It is represented by a series of stratified sands and clays of various colors, with beds of silicious gravel, often cemented into a ferrugin- ous conglomerate by the infiltration of a hydroxyd of iron. In some places it contains green, marly sand, with casts of fossils, and along the edge of the Ohio, at extreme low water, at Caledonia, there is a thin bed of lignite. At Fort Massac, just above Metropolis, the fer- ruginous conglomerate is from forty to fifty feet in thickness. Near Caledonia, a section gave a thickness of 564 feet. T, A. Conrad+ described, from the Miocene of the Eastern and Southern States, Nassa subcylindrica, Volutifusus typus, Cancellaria scalarina, Saxicava parilis, Spisula capillaria, Tellina peracuta, T. capillifera, Astarte compsonema, Lithophaga subalveata, Macoma virginiana, Mercenaria obtusa, and Cumingia medialis. | Philip P. Carpenter{ described, from the Pliocene of Santa Barbara, California, Turritella jewetti, Bittium armillatum, Opalia insculpta, Trophon tenuisculptus, and Pisania fortis. In 1867, Prof. E. W. Hilgard§ said that nowhere has the geologist more need of divesting himself of reliance upon lithological characters, than in the study of the Mississippi Eocene. Not only do the materials of the different groups often bear a most extraordinary resemblance to each other, but their character varies incessantly, in one and the same stratum, within short distances. Hale remarks that in Mississippi, the Orbitoides limestone seems to be represented by blue marlstone, and so itis, sometimes. But while on the one hand we see the hard limestone of the Vicksburg bluff passing into blue marl (Byram, Marshall’s quarry ), we on the other hand find it passing equally into a rock undistinguishable from that of St. Stephens (Brandon, Wayne county) ; the varied fossils described by Conrad disappearing almost = Geo. Sur. of Tll., vol. 1. + Am. Jour. Conch., vol. ii. tf Ann. & Mag. Nat. Hist., 3d ser., vol. xvii. § Am. Jour. Sci. & Arts, 2d ser., vol. xliii. ‘ 26 Cincinnati Society of Natural History. entirely, to be replaced by millions of Orbitoides imbedded in a semi- indurate mass of carbonate of lime, interspersed at times with similar- ly constituted conglomeratic masses of Pecten poulsoni. He could not, therefore, agree to the propriety of distinguishing as separate divisions the Orbitoides limestone, and the Vicksburg Group. The occurrence of a different species of Orbitoides (O. nupera) at Vicksburg, does not. alter the case, for the undoubted O. mantelli occurs there also, in the solid rock. And there are few of the characteristic fossils of the Vicksburg profile, which do not, on some occasions, occur side by side with the O. mantelli, and its companions, Pecten poulsoni, and Ostrea vicksburgensis. Of course, the coral had its favorite haunts—the mollusks theirs. There is nothing surprising in the fact, that where one abounds, the others are usually scarce, or vice versa. He regarded the Shell Bluff Group of Conrad, or the Red Bluff Group— No. 4 of the Vicksburg section—which is characterized by the occur- rence of Ostrea georgiana, as more or less co-extensive with the Vicks- burg Group, and regularly associated with it, asa subordinate feature. Its inconsiderable thickness readily explains its entire absence at — many points, where, stratigraphically, it ought to appear. Prof. E, D. Cope* described, from the Miocene of Charles county, Maryland, Lschrichtius cephalus, Rhabdosteus latiradix, Squalodon mento, Aetobatis profundus, Myliobatis gigas, M. pachyodon, M. vi- comicanus, Raja dux, Notidanus plectrodon, Galeocerdo levissimus, Sphyrna magna, Trionyx celiulosus, Thecachampsa contusor, T. seri- codon, Orycterocetus crocodilinus, Priscodelphinus acutidens, Esch- richtius leptocentrus, Squalodon protervus, and Galera macrodon. T. A. Conrad+ described, from the Eocene of Texas, Venericardia | mooreana; from the Miocene of the Eastern and Southern States, Plew- romeris decemcostata, Mactra contracta, M. virginiana, Lucina den- sata, Cardium emmonsi, Mercenaria percrassa, Mulinia parilis, Semele carolinensis, Abra nuculiformis, Corbula curta, Pecten tricari- natus, P. yorkensis, Sycotypus pyriformis, Cylichna, virginica, Zizy- phinus briant, Z. punctatus, Neverita densata, N. emmonst, Ptycho- salpinx, scalaspira, Paranassa granifera, Bursa centrosa, and Busy- con dumosum. Prof. Gill described, from North Carolina, Sycotypus elongatus. ) In 1868, Prof. J. W. Dawsont offered the following reasons, to show, * Proc. Acad. Nat. Sci. + Am. Jour. Conch., vol. iii. { Acadian Geology. Mesozoic and Cenozoic Geology and Paleontology. 27 that the drift deposits of eastern America are not to be accounted for ‘upon the theory of a terrestrial origin or a supposed glacial period. ° 1. It reqnires a series of suppositions unlikely in themselves, and not warranted by facts. The most important of these is the coincidence of a wide-spread continent, and a universal covering of ice in a temperate latitude. In the existing state of the world, it is well known that the ordinary conditions required by glaciers in temperate latitudes are elevated chains and peaks extending above the snow-line; and that cases, in which, in such latitudes, glaciers extend nearly to the sea level, occur only where the mean temperature is reduced by cold ocean currents approaching to high land, as for instance, in Terra del Fuego, and the southern extremity of South America. But the temperate re- gions of North America could not be covered with a permanent mantle of ice under the existing conditions of solar radiation; for, even if the whole were elevated into a table-land, its breadth would secure a suf- ficient summer heat to melt away the ice, except from high mountain peaks. Either, then, there must have been immense mountain-chains which have disappeared, or there must have been some unexampled as- tronomical cause of refrigeration, as, for example, the earth passing into a colder portion of space, or the amount of solar heat being dim- inished. But the former supposition has no warrant from geology, and astronomy affords no evidence for the latter view, which, beside, would imply a diminution of evaporation, militating as much against the glacier theory as would an excess of heat. An attempt has recently been made by Professor Frankland to account for such a state of things, by the supposition of a higher temperature of the sea, along with a colder temperature of the land; but this inversion of the usual state of things is unwarranted by the doctrine of secular cooling of the earth; it is contradicted by the fossils of the period, which show that the seas were colder than at present; and ifit existed, it could not produce the effects required, unless a preter-natural arrest were at the same time laid on the winds, which spread the temperature of the sea over the land. The alleged facts observed in Norway, and stated to support this view, are evidently nothing but the results ordinarily observed in ranges of hills, one side of which fronts could sea-water, and the other land warmed in summer by the sun. The supposed effects of the varying eccentricity of the earth’s orbit, so ably expounded by Mr. Croll, are no doubt deserving of considera- tion in this connection; but I agree with Sir Charles Lyell in regard- ing them as insufficient to produce any effect so great as that refrigera- 28 Cincinnati Society of Natural History. tion supposed by the theory now before us, even if aided.by what Sir Charles truly regards as a more important cause of cold—namely, a- different distribution of land and water, in such a manner as to give a great excess of land in high latitudes. 2, It seems physically impossible that a sheet of ice, such as that supposed, could move over an uneven surface, striating itin directions — uniform over vast areas, and often different from the present inclina- tions of the surface. Glacier ice may move on very slight slopes, but it must follow these ; and the only result of the immense accumulation of ice supposed, would be to prevent motion altogether by the want of slope or the counter-action of opposing slopes, or to induce a slight and irregular motion toward the margins, or outward from the more prominent protuberances. It is to be observed, also, that, as Hopkins has shown, it is only the sliding motion of glaciers that can polish or erode surfaces, and that any internal changes, resulting from the mere weight of a thick mass of ice resting on a level surface, could have little or no influence in this way. . 3. The transport of bowlders to great distances, and the lodgment of them on hill-tops, could not have been occasioned by glaciers. These carry downward the blocks that fall on them from wasting cliffs. But the universal glacier supposed could have no such cliffs from which to collect ; and it must have carried bowlders for hundreds of miles, and left them on points as high as those they were taken from. On the Montreal Mountain, at a height of 600 feet above the sea, are huge bowlders of feldspar from the Laurentide Hills, which must have been carried 50 to 100 miles from points of scarcely greater elevation, and over a valley in which the striz are in a direction nearly at right angles with that of the probable driftage of the bowlders. Quite as striking examples occur in many parts of the country. It is also to be observed that bowlders, often of large size, occur scattered through the marine stratified clays and sands containing sea-shells ; and what- ever views may be entertained as to other bowlders, it can not be denied that these have been borne by floating ice. Nor is it true, as has been often affirmed, that the bowlder clay is destitute of marine fossils. At Isle Verte, Riviere du Loup, Murray Bay, and St. Nicholas on the St. Lawrence, and also at Cape Elizabeth, near Port- land, there are tough stony clays of the nature of true “till,” and in_ the lower part of the drift, which contain numerous marine shells of the usual Post-pliocene species, po . ae 4 te Mesozoic and Cenozoic Geology and Paleontology. 29 4, The Post-pliocene deposits of Canada, in their fossil remains and general character, indicate a gradual elevation from a state of depres- sion, which on the evidence of fossils must have extended to at least 500 feet, and on that of far-traveled bowlders to several times that amount; while there is nothing but the bowlder clay to represent the previous subsidence, and nothing whatever to represent the supposed previous ice-clad state of the land, except the scratches on the rock surfaces, which must have been caused by the same agency which de- posited the bowlder clay. 5. The peat deposits, with fir roots, found below the bowlder clay in Cape Breton, the remains of plants and land snails in the marine clays of the Ottawa, and the shells of the St. Lawrence clays and sands, show that the sea at the period in question had nearly the tem- perature of the present Arctic currents of our coasts, and that the land was not covered with ice, but supported a vegetation similar to that of Labrador and the north shore of the St. Lawrence at present. This evidence refers not to the later period of the Mammoth and the ‘Mastodon, when the re-elevation was perhaps nearly complete, but to the earlier period contemporaneous with, or immediately following the supposed glacier period. In my former papers on the Post-pliocene of the St. Lawrence, I have shown that the change of climate involved is not greater than that which may have been due to the subsidence of land, and to the change of the course of the Arctic current, actually proved by the deposits themselves. It has long been known to geologists, that in northeastern America, two main directions of striation of rock surfaces occur, from north- east to southwest, and from northwest to southeast; and that locally the directions vary from these to north and south, and east and west. It would seem that the dominant direction in the valley of the St. Lawrence, along the high lands to the north of it, and across western New York, is northeast and southwest; and that there is another series of scratches running nearly at right angles to the former, across the neck of land between Georgian Bay and Lake Ontario, down the valley of the Ottawa, and across parts of the eastern townships, con- necting with the prevalent south and southeast striation, which occurs in the valleys of the Connecticut and Lake Champlain, and elsewhere in New England, as well as in Nova Scotia and New Brunswick. What were the determining conditions of these two courses, and were they contemporaneous or distinct in time? The first point to be set- tled in answering these questions is the direction of the force which 30 Cincinnati Society oy Natural History. caused the striz. Now, I have no hesitation in asserting, from my own observations, as well as from those of others, that for the south- west striation the direction was from the ocean toward the interior, against the slope of the St, Lawrence valley. The crag-and-tail forms of all our isolated hills, and the direction of transport of bowl- ders carried from them, show that throughout Canada the movement was from northeast to southwest. ‘This at once disposes of the glacier theory for the prevailing set of strie; for we can not suppose a glacier moving from the Atlantic up into the interior. On the other hand, it is eminently favorable to the idea of ocean drift. A subsi- dence of America, such as would at present convert all the plains of Canada and New York and New England into sea, would determine the course of the Arctic current over this submerged land from north- east to southwest; and as the current would move up @ slope, the ice which it bore would tend to ground, and to grind the bottom - as it passed into shallower water; for it must be observed that the character of slope which enables a glacier to grind the surface amy prevent ice borne by a current from doing so, and vice versa, Now. we know that in the Post-pliocene period, eastern America was submerged, and, consequently, the striation at once comes into har- mony with other geological facts. We have, of course, to suppose that the striation took place during submergence, and that the process was slow and gradual, beginning near the sea and at the lower levels, and carried upward to the higher ground in successive centuries, while the portions previously striated were covered with deposits swept down from the sinking land or dropped from melting ice. The predominant southwest striation, and the cutting of the upper lakes, demand an outlet to the west for the Arctic current. But both during depression and elevation of the land, there must have been a time when this ovtlet was obstructed, and when the lower levels of New York, New England and Canada were still under water. Then the valley of the Ottawa, that of the Mohawk, and the low country between Lakes Ontario and Huron, and the valleys of Lake Champlain and the Connecticut, would be straits or arms of the sea, and the current, ob- structed in its direct flow, would set principally along these, and act on the rocks in north and south and northwest and southeast directions. To this portion of the process, I would attribute the northwest and southeast striation. It is true, that this view does not account for the southeast striz observed on some high peaks in New England; but it must be observed that even at the time of greatest depression, the Arc- ay? up lebs . ae : t sr Mesozoic and Cenozoic Geology and Paleontology. 3l tic current would cling to the Northern land, or be thrown so rapidly to the west that its direct action might not reach such summits. Nor would I exclude altogether the action of glaciers in eastern America, though I must dissent from any view which would assign to them the principal agency in our glacial phenomena. Under a condi- tion of the continent in which only its higher peaks were above the water, the air would be so moist, and the temperature so low, that per- manent ice may have clung about-mountains in the temperate latitudes. The striation itself shows that there must have been extensive glaciers, as now, in the extreme Arctic regions. Yet I think, that most of the alleged instances must be founded on error, and that old sea-beaches have been mistaken for moraines. I have failed to find even in our higher mountains any distinct sign of glacier action, though the action of the ocean breakers is visible almost to their summits; and though I have observed in Canada and Nova Scotia many old sea-beaches, eravel-ridges, and lake-margins, I have seen nothing that could fairly be regarded as the work of glaciers. The so-called moraines, in so far as my observation extends, are more probably shingle beaches and bars, old coast-lines loaded with bowlders, trains of bowlders or “ ozars.”’ Most of them convey to my mind the impression of ice-action along a slowly subsiding coast, forming successive deposits of stones in the shal- low water, and burying them in clay and smaller stones as the depth increased. These deposits were again modified during emergence, when the old ridges were sometimes bared by denudation, and new ones heaped up. We now have, in all, exclusive of doubtful forms, about one hundred species of marine invertebrates, from the Post-pliocene clays of the St. Lawrence valley. All, except four or five species, belonging to the older or deep. water part of the deposit, are known as living shells of the Arctic or boreal regions ofthe Atlantic. About half of the species are fossil in the Post-pliocene of Great Britain. The great majority are now living in the Gulf of St. Lawrence, and on the neighboring coasts;-and more especially on the north side of the gulf and the coast of Labrador. In so far, then, as marine life is concerned, the modern period in this country is connected with that of the bowlder clay by an unbroken chain of animal existence, These deposits in Lower Canada afford no indications of the terrestrial fauna ; but the remains of Hlephus primigenius, in beds of similar age in Upper Canada, show that during the period in question, great changes occurred among the animals of the land ; and we may hope to find similar evidences else- 32 Cincinnati Society of Natural History. where, especially in localities where, as on the Ottawa, the debris of land-plants and land-shells occur in the marine deposits. The Eocene of New Jersey* is known as the Upper marl bed, and has a thickness of 37 feet. Fossils are abundant wherever marl pits have been opened, between Deal on the sea shore and Clementon in Camden county. The Miocene is recognized by its fossils in many localities in New Jersey. It is not always conformable with the Eocene below, and its thickness is variable. In 1868, Prof. E. D. Cope} described the Miocene deposit of the western shore of Maryland, as consisting of a dark, sandy clay, vary- ing from a leaden to a blackish color, through which water does not penetrate. Its upper horizon may be traced along the high shores and cliffs of the Chesapeake by the line of trickling springs’ which follow its upper surface. A great bed of shells occurs at from fourteen to twenty-two feet below its upper horizon. He described, Cetophis heteroclitus, Ixacanthus celospondylus, Pris- codelphinus spinosus, now Belosphys spinosus, P. atropius, now B. atropius, P. stenus, now B. stenus, Zarhachis flagellator, Delphin- apterus ruschenbergert, now Tretosphys ruschenbergert, D. lacertosus, now 7’. lacertosus, D. gabbi, now T. gabbi, D. hawkinsi, now T. hawkinst, D, tyrannus, now LEschrictius tyrannus, E. pusillus, Megaptera expansa, now H. expansus; from the Eocene green sand of Monmouth county, New Jersey, Paleophis halidanus, and P. littoralis. Isaac Lea described, from a Miocene deposit, six miles northeast of Camden, New Jersey, Unio alatoides, U. carriosoides, U. humerosot- des, U. nasutoides, U.radiatoides, U. subrotundoides, U. roanokoides, U. ligamentinoides, U. grandioides, and U. corpulentoides. Dr. Joseph Leidy described, from blue clay and sand beneath a bed of bitumen of Pliocene age, in Hardin.county, Texas, Megalonyx vali- dus, Trucifelis fatalis, and Emys petrolec; from Douglas Flat, Calav- eras county, California, Hlotherium superbum; from Martinez, #quus pacificus, the largest known fossil horse tooth; from Ashley river, South Carolina, Hoplocetus obesus; from Gibson county, Indiana, Di- cotyles nasutus, found when digging a well between 30 and 40 feet be- low the surface: from the Miocene of the Bad Lands of White river, Dakota, Leptictis haydeni, Ictops dakotensis; from Half-mvon Bay * Geo. of N. Jersey, 1868. } Proc. Acad. Nat. Sci. Mesozoic and Cenozoic Geology and Paleontology. 30 California, Delphinus occidwus; from Washington county, Texas, An- chippus texanus; from the Bad Lands of Nebraska, Lophiodon occiden- tale, and from Shark river, Monmouth county, New Jersey, Anchippo- dus riparius. T. A. Conrad* described, from the Miocene of the Atlantic coast, Volutella oviformis, Prunum virginiana, now. Marginella virginiana, Mercenaria cuneata, Caryatis plionema, Carditamera recta ; and from Wyoming, Goniobasis cartert. Prof. O. C. Marsh} described, from the Tertiary at Antelope station, on the Union Pacific Railroad, 450 miles west of Omaha, in Nebraska, Hquus parvulus, now Protohippus parvulus. The Tertiary underlies a wide central belt in West Tennessee, and was subdivided by Prof. Safford,{ in 1869, in ascending order, into 1, Porters’ Creek Group ; 2, Orange Sand; 3, Bluff Lignite ; 4, Post- pliocene beds, on the Mississippi Bluff, consisting of Bluff gravel and Bluff loam ; and superficial gravel beds, in other parts of the State, consisting of ore-region gravel, eastern gravel, and lastly of bottoms, and alluvial beds. The Bluff lignite consists, especially in the middle and southern parts of the State, ofa series of stratified sands, with more or less sandy, slaty clay, characterized by the presence of well-marked beds of lignite; though, in the northern part of the State, its upper portion is frequently more or less indurated, presenting layers of soit sand- stone with less lignite. The upper part of the series is generally well exposed below the gravel of the Mississippi Bluffs. At Memphis, how- ever, it scarcely appears above low-water. About one hundred feet of the series has been seen. . In this thickness it contains from one to three beds of lignite, which are from half a foot to four feet in thickness. The outcrop of the Orange sand or Lagrange Group, forms more than athird of the entire surface of West Tennessee. It occupies a belt, about 40 miles wide, which runs in a northeasterly direction, through nearly the central portion of this division of the State. As seén in bluffs, railroad cuts, gullies, and in nearly all exposures, it is generally a great stratified mass of yellow, orange, red or brown, and white sands, presenting occasionally an interstratified bed of white, * Am. Jour. Conch., vol. iv. ft Am. Jour. Sci. & Arts, 2d series, Vol. xlvi. t Geo. of Tenn. 34 Cincinnati Society of Natural History. grey, or variegated clay. The sand beds are usually more or less argillaceous ; sometimes but little, or not at all so. Like the Ripley Group, it contains, occasionally, patches, plates, and thin layers of ferruginous, sometimes argillaceous sandstone, and as in that group, presents, locally, massive blocks of sandstone on high points. At La Grange, a fine section of the group, more than a hundred feet in . thickness, is exposed. It includes within its outcrop, nearly all of Fayette, Haywood, Madison, Gibson, and Weakley counties; the larger parts of Hardeman, Carroll, and Henry ; and small parts of Shelby, Tipton, Henderson, Dyer, and Obion. He supposed this group to be of Eocene age, and to have a thickness of about 600 feet. This group must not be confounded with the Post-pliocene Orange sand of Hilgard, which occurs in Mississippi and Louisiana. The Porter’s Creek Group contains proportionally more laminated or slaty clay than the Orange Sand or Lagrange Group. Along the Mem- phis and Charleston railroad, the belt of surface occupied by the group is about eight miles wide. It becomes narrower in its north- ward extension, and appears to be the northern extension of the lower part of Hilgard’s Northern Lignitic Group. The thickness is from 200 to 300 feet, and in this are usually several beds of slaty clay from five to fifty feet in thickness. It is well exposed on Porter’s creek, in Hardeman county, and on the road from Bolivar to Purdy, commence- ing about seven miles from the former place, and extending to or be- yond Wade’s creek. Prof. E. W. Hilgard* described the Grand Gulf Group, Orange Sand and Loess at Port Hudson, Miss., and gave a descending section midway between Port Hudson and Fontania as follows: Ist, Yellow loam, sandy below, 8 to 10 feet. 2d, White and yellow hard pan, 18 feet. 3d, Orange and yellow sand, sometimes ferruginous sandstone, irregularly stratified, 8to15 feet. 4th, Heavy, greenish or bluish clay, 7 feet. 5th, White, indurate silt or hard pan, 18 feet. 6th, Heavy, green clay, with porous, calcareous concretions above, ferruginous ones below; some sticks and impressions of leaves, 30 feet. 7th, Brown muck and white or blue clay with cypress stumps, 3 to 4 feet. At the stage of extreme low water the stump stratum is visible to the thickness of 10 feet at its highest point; showing several genera- tions of stumps, one above another, also the remnants of many succes- sive falls of leaves and overflows. The wood is in a good state of * Am. Jour. Sci. & Arts, 2d series, vol. xlvii. Mesozoic and Cenozoic Geology and Paleontology. 35 preservation. The stump stratum exists, at about the same level, over all the Delta plain of the Mississippi and along the Gulf coast from Mobile, on the east, to the Sabine river. Dr. Joseph Leidy* described, from the White River Group of Dakota, Oreodon affinis, O. bullatus, O. hybridus, Leptauchenia nitida, Homo- camelus caninus, Cosoryx furcatus, Nanohyus porcinus, Protohippus placidus, Hipparion affine, and H. gratum, He described from the Eocene near Fort Bridger, Wyoming,t Omomys carteri, Trionyx guitatus, Emys wyomingensis, and from South Bitter creek, near where it crosses the stage route, 70 miles west of the summit of the Rocky mountains, in western Wyoming, Crocodilus aptus. Prof. E. D. Copet described, from the Miocene of Shiloh, Cumber- land county, New Jersey, Zretosphys ureus, Zarhachis velox, and Trionyx lima; from the mouth of the Patuxent river, Maryland, Zarhachis tysont. He described,§ from the Eocene marl pits, at Shark river, Monmouth county, N. J., Hemicaulodon effodiens; from Farmingdale, Myliobates glottoides, and Celorhynchus acus; from the Green River Group, on the upper waters of Green river, Wyoming, Asineops squamifrons, Clupea pusilla, Cyprinodon levatus; from the Miocene in Wayne county, North Carolina, Pnewmatosteus nahunticus; from Duplin county, Pristis attenuatus; from Edgecombe county, Hschrichtius polyporus; from Quanky creek, Halifax county, Mesoteras kerranus; from Stafford county, Va., Thinotherium annulatum. He described, from the Post-pliocene, at Savannah, Georgia, Anoplo- nassa forcipata; from cave Breccia, in Wythe county, Virginia, Zamias levidens, Sciurus panolius, and Galera perdicida. Prof. O. C. Marsh|| described, from the Eocene, near Shark river, Monmouth county, New Jersey, Dinophis grandis. T. A. Conrad described, from the same locality, Pecten kneiskerni, Crassatella littoralis, Crassina veta, Bucardia veta, Caryatis dela- warensis, Protocardia curta, Onustus annosus, and Terebratula glossa, And from the Miocene of St. Charles county, Maryland, and from Petersburg, Va., Pecten cerinus, Callista virginiana, Saxicava insita, Scapharca tenuicardo, Mercenaria plena, and Capsa parilis. * Jour. Acad. Nat. Sci., vol. vii. + Proc. Acad. Nat. Sci. t Proc. Acad. Nat. Sci. 2 Proc. Am. Phil. Soe., vol. xi. || Am- Jour. Sci. & Arts, 2d series, vol. xlviii. 7 Am. Jour. Conchology, vol. v. 36 Cincinnati Society of Natural History. W. M. Gabb* described, from the Miocene in Contra Costa county, near Tomales bay, near Martinez, Walnut creek, Monterey ~ county, San Emidio, Cerros island, and other: places in California, Dosinia mathewsonit, Pecten packhami, Triptera clavata, Trophon ponderosum, Neptunea recurva, Metula remondi, Agasoma gravida, A. sinuata, Ranella mathewsoni, now Bursa mathewsoni, Cuma” biplicata, Ancillaria jfishi, Neverita callosa, Cancellaria vetusta, Turritella hoffmanni, Trochita jilosa, T. inornata, Pachypoma biangulata, Pandora scapha, Hemimactra lenticularis, H. occiden- talis, Schizodesma abscissa, Chione mathewsoni, now Callista mathewsoni, C. whitneyt, now C. whitneyt, Callista voyt, Dosinia conradi, Tapes truncata, Cardium meekanum, Conchocele disjuncta, Mytilus mathewsont, Modiola multiradiata, now Volsella multi- radiata, Pecten cerrocensis, P. veatchi, Ostrea atwoodi, O. taylorana, O. veatchi, O. cerrocensis, Asterias remondi, Ficus pyriformis, F. — nodiferus, Venus pertenuis. From the fresh water Tertiary, or Plio- cene, on Snake river, in Idaho Territory, Melania taylori, and Lithasia antiqua ; from the Pliocene, near Santa Barbara, Humboldt bay, San Francisco county, Kirker’s Pass, Sonoma county, and other places in California, Cancer brewert, Surcula carpenterana, Pleuro- soma voyt, Columbella richthofeni, Littorina remondi, Zirphea dentata, Gari alata, Dosinia staleyi, now Tapes staleyi, Cyrena californica, Lucina richthofeni, Neptunea altispira, N. humerosa, Sigaretus planicostum, Cancellaria altispira, Acmea rudis, Siliqu- aria edentula, Caryatis barbarensis, Saxidomus gibbosus. And from the Post-pliocene, near Santa Barbara, and San Pedro, Surcula tryonana, S. perversa, Clathurella conradana, Muricidea paucivari- cata, Trophon squamutifer, Cancellaria gracilior, and C. tritonidea. Prof, Leo. Lesquereux} described,from the Lower Eocene or Northern Lignitic Group of Tippah, Miss., and La Grange, and Sommerville, Tennessee, Calamopsis danai, Sabal grayana, now Sabalites grayanus, Salisburia binervata, Populus monodon, Salix worthent, S. tabellaris, Quercus moort, Y. retracta, Celtis brevifolia, Ficus schimperi, fF. cin- namomoides, Laurus pedatus, Cinnamomum mississippiense, Persea lancifolia, Ceanothus meigsi, Juglans appressa, J. saffordana, Mag- nolia laurifolia, M. lesleyana, M. ovalis, M. cordifolia, Asimina leiocarpa, and Phyllites truncatus. * Pal. of Cal., vol. ii. + Trans. Am. Phil. Soc., vol. xiii. Mesozoic and Cenozoic Geology and Paleontology. 37 Oswald Heer* described, from the Tertiary of Alaska, Pteris sitken- sis, Taxodium tinajorum, Taxites microphyllus, Phragmites alaskanus, Poacites tenuistriatus. Carex servata, Sagittaria pulchella, Vaccinium Sriest, Diospy ros stenosepala, Viburnum nordenskioldi, Hedera auri- culata, Vitis crenata, Tilia alaskana, celastrus borealis, Ilex insig- nis, Trapa borealis, Juglans nigella, J. picroides, Spirea andersoni, and identified numerous plants with those described from the Miocene of Europe. He described the insect Chrysomelites alaskanus, and Dr. Carolus Mayer described, Unio onariotis, U. athlios, Paludina abavia, and Melania furuhjelmi. The Jackson Group, in Louisiana,+ consists of marine strata; of lig- nitic beds that tell of swamps; and of nonfossiliferous beds of lamin- ated sands and clays. It spreads over the State north of the Vicks- burg outcrop and west of the Bastrop Hills. The marine strata con- tain massive clays, often full of selenite. At Grand View there is a stratum of such clay 85 feet thick. The Vicksburg Group, in Louisiana, consists of smooth, yellow and red clays, with a very small proportion of sand. Limestone no- dules occur, generally, soft and yellow, but sometimes hard and white, and always full of casts of shells. It is exposed from Godwin’s shoals to about six miles south of Natchitoches, and from a point below Montgomery to the Washita, below Grand View, but if never occupies an area more than about twelve miles wide. | In 1870, Dr. Joseph Leidyt described, from the Fort Bridger Eocene, of Wyoming, Baptemys wyomingensis, now Dermatemys wyoming- ensis, Hmys stevensonanus, Patriofelis ulta, Lophiodon modestus, Hyopsodus paulus, mys jeansi, FE. haydeni, Baena arenosa, Saniva ensidens ; from near the junction of the Big Sandy and Green rivers, Paleosyops paludosus, Orocodilus elliott’; from Black’s Fork, Microsus cuspidatus, Notharctus tenebrosus; from the Tertiary of Colorado, Megacerops coloradoensis ; from the Tertiary of the Rocky mountain region, Oncobatis pentagonus, Mylocy- prinus robustus ; from Henry’s Fork of Green river, Lophiotherium sylvaticum ; from the Miocene in the valley of Bridge creek, a tributary of John Day’s river, Oregon, Oreodon superbus, Anchitherium condoni ; from Gay Head, Martha’s Vineyard, Graphiodon vinearius ; from the * Flora Fossilis Alaskana. + Geo. of Louisiana, 1870. t Proc. Acad. Nat. Sci. 38 Cincinnati Society.of Natural History. Pliocene of the Niobrara river, Merychocherus rusticus ; from Dry creek, Stanislaus county, California, Mastodon shepardi ; and from Tuolumne county, Auchenta californica. Prof. O. C. Marsh* described, from the Eocene of New Jersey, The- cachampsa minor; from the Miocene of Edgecombe county, North Car- olina,t Catarractes antiquus; from Maryland, Puffinus conradi; from the Niobrara river, Grus haydeni, Graculus idahensis; from Squan- kum, New Jersey,{ Rhinoceros matutinus; from Shark river, Dicotyles antiquus; and from the Pliocene at Monmouth, Meleagris altus. Prof. F. B. Meek described, from the Miocene, at Fossil Hill, Hot Spring mountains, Idaho, Spherium rugosum, S. idahoense, Ancylus undulatus, Goniobasis sculptilis, G. subsculptilis, Carinifex binneyt, C. concava and C. tryoni. T. A. Conrad§ described, from the Miocene of Virginia and South Carolina, Artena undulata, Crepidula rostrata, C. recurvirostra, C. virginica, Persicula ovula, aud Axinea bella. The Grand Gulf Group of Louisiana|| consists of nonfossiliferous clays and sandstones pretty regularly stratified, varied, occasionally, by clayey sand and beds containing twigs and leaves. The sandstone oc- curs in ledges from six inches to 20 feet in thickness. It is cut into four parts by the bluff and the alluvion of Red river and the Missis- sippi. One reaches the Vicksburg area and extends into Missis- sippi; another is southwest of Red river and extends into Texas; an- other is northeast of Red river as far as Sicily Island on the Ouachita; and the other is at the western part of the Avoyelles prairies. In 1871, T. A. Conrad@ described, from the Eocene at Claiborne, Alabama, Caryatis exigua; and from the Oligocene at Vicksburg, Mississippi, Macoma sublintea, and Abra protexta. F. B. Meek** described, from the Bridger Eocene at Henry’s Fork, Black’s Fork, and Church buttes, Wyoming, Viviparus wyomingensis. Brady and Crosskeyt++ described, from the Post-pliocene of Port- land and Saco, Maine, and from Montreal, Canada, Cythere mac- chesneyi, C. loganit, C. cuspidata,. Cytherura cristata, C. granulosa, and Oytheropteron complanatum. * Am. Jour. Sci. and Arts, 2d series, vol. 50. + Ibid, vol. xlix. t Proc, Acad. Nat. Sci. § Am. Jour. Conch., vol. vi. || Geo. of Lou., 1871. 7 Am. Jour. Conch., vol. vi. ** Proc. Acad. Nat. Sci. t+ Lond. Geo. Mag., vol. viii. a. Mesozoic and Cenozoic Geology and Paleontology. 39 Dr. Joseph Leidy* described, from the Bridger Eocene of Wyoming, Anosteira ornata, Hybemys arenarius, Testudo corsoni, Emys carteré, Baena undata, Trogosus vetulus, now Anchippodus vetulus, Sinopa rapax, Paleosyops major, Hyrachyus eximius, Paramys delicatus, P. delicatior, and P. delicatissimus, all now Plesiarctomys, and Mysops minimus. He described from the Miocene of Alkali flats, Oregon, Rhinoceras pacificus, and from Crooked river, Stylemys oregonensis, now Testudo oregonensis. Prof. E. D. Copey described, from the Post-pliocene occurring in a limestone fissure in Chester county, Pennsylvania, Megalonyx loxodon, M. sphenodon, M. tortulus, M. wheatleyi, Sciurus calycinus, Arvicola speothen, A. tetradelta, A. didelta, A. involuta, A. sigmodus, A. hiatt- dens, Erithizon cloacinum, and Praotherium palatinum.- He described from the Miocene near Tuxtla, Chiapas, Mexico, Prymnetes longiven- ter. Prof. O. C. Marsht{ described, from the Green river basin west of the Rocky Mountains, Boavus agilis, B. brevis, and B. occidentalis; from ' the Bridger Eocene of Wyoming, Limnophis crassus, Lithophis sar- genti, Crocodilus affinis, C. brevicollis, C. grinnelli, C. liodon, C. zipho- don, now Limnosaurus ziphodon, Glyptosaurus anceps, G. nodosus, G. ocellatus, G. sylvestris, Titanotherium (?) anceps, Lophiodon affinis, L. bairdianus, L.nanus, L. pumilis, Anchitherium gracile, now (?) Orohip- pus gracilis, Lophiotherium ballardi, Hlotherium lentum, Platygonus zieglert, Hyopsodus gracilis, Limnotherium elegans, L. tyrannus, Sct- uravus nitidus, S. parvidens, S. undans, Triacodon fallax, Canis mon- tanus, Vulpavus palustris, and Bubo leptosteus. He described from the Miocene at Scott's Bluff, on North Platte river, Nebraska, Amphicyon angustidens; from Northern Colorado, Meleagris antiquus; from Cumberland county, New Jersey,§ Lophio- don validus, now Tapiravus validus; and named, but did not describe, from Wyoming, Amu depressa, A. newberryana, Lepidosteus glaber, and LZ. whitney. Also from the Pliocene sands, near the headwaters of the Loup Fork river, Nebraska, (||) Platygonus striatus, Arctomys vetus, Geomys bisuicatus, Aquila dananus; and from Oregon, Platy- gonus condonit, and Dicotyles hesperius. * Proc. Acad. Nat. Sci. + Proc. Am. Phil. Soc., vol. xii. t Am. Jour. Sci. and Arts, 3d series, vol. i. & il. § Proc. Acad. Nat. Sci. (||) Am. Jour. Sci. and Arts, 3d series, vol. ii. 40 Cincinnati Society of Natural History. In 1872, Dr. Dawson* said, that the Bowlder clay of Canada con- sists of hard, gray clay, filled with stones, and thickly packed with bowlders, and usually rests directly on striated rock surfaces ; though in Cape Breton, a peaty or brown coal deposit, with branches of trees, has been found to underlie it, and in some places there are deposits of rolled gravel beneath it. The stones are often scratched and ground into wedge-shapes, as if by the action of ice. At Isle Verte, Riviere du Loup, Murray Bay, Quebec, and St. Nicholas, on the St. Lawrence it is fossilferous, containing, Leda truncata, Balanus hameri, and Bryozoa. In some localities the stones in the Bowlder clay, are alions exclu- sively those of the neighboring rock formations, in others those having traveled from a distance predominate ; occasional instances occur’ where bowlders have been transported to the northward. Though the Bowlder clay often presents a somewhat widely extended and uniform sheet, yet it may be stated to fill up small valleys or depressions, and to be thin or absent on ridges and rising grounds. Beneath the Bowlder clay on the St. Lawrence and the Ottawa, there are two sets of striz, a southeast set, and a southwest set. In Nova Scotia and New Brunswick, as in New England, the prevailing direc- tion, is southeastward, though there are’ also southwest and south striation, and a few cases where the direction is nearly east and west. At the Mile end quarries, near Montreal, the polished and grooved surface of the limestone, shows four sets of striz. The principal ones have the direction of S. 68° W. and S. 60° W. respectively, and the second of these sets isthe stronger and coarser, and sometimes oblit- erates the first. ‘The two other sets are comparatively few and feeble strize, one set running nearly north and south, and the other northwest and southeast. ‘These last are probably newer than the first two sets. The locality is to the northeast of the mass of trap constituting the Montreal mountain, and evinces that the movement must have been up the St. Lawrence, which is the dominant direction of the striz in this valley. It is the Bowlder clay connected with this 8. W. striation, that is rich in marine fossils. At the mouth of the Saguenay, near Moulin Bode, are striz and grooves on a magnificent scale, some of the latter being ten feet wide, and four feet deep, cut into hard gneiss. Their course is N. 10° W. . to N. 20° W. magnetic, or N. 30° to 40° W. when referred to the true * Post-pliocene Geol. Mesozoic and Cenozoic Geology and Paleontology. Al meridian. In the same region, on hills 300 feet high, are roches moutonnees with their smoothest faces pointing in the same direction, or to the northwest. his direction is that of the valley or gorge of the Saguenay, which enters nearly at right angles the valley of the St. Lawrence. In like manner at Murray Bay, there are striz on the Silurian lime- stones near Point au Pique, which run about N. 45° W., but these are crossed by another set having a course 8. 30° W., so that we have two sets of markings, the one pointing upward along the deep valley of Murray Bay river to the Laurentide hills inland, the other following the general trend of the St. Lawrence valley. The Bowlder clay which rests on these striated surfaces, is a dark-colored till, full of Laurentian bowlders, and holding Leda truncata, and also Bryozoa clinging to some of the bowlders. In ascending the Murray Bay river, we find these bowlder beds surmounted by very thick, stratified clays, with marine shells, which extend upward to an elevation of about 800 feet, when they give place to loose bowlders and unstratified drift. The Bowlder clay over a large portion of the plain of Lower Canada is succeeded by the Leda clay, which varies in thickness from a few feet to 50 or perhaps 100 feet. The material of the Leda clay is of the same nature as the finer portion of the paste of the Bowlder clay, and the latter seems to graduate into the former. It sometimes holds hard, calcareous concretions, which, as at Green’s creek, on the Ottawa, are occasionally richly fossiliferous. When dried, the Leda clay be- comes of stony hardness, and when burned, it assumes a brick red col- or. When dried and levigated, it nearly always affords some foramin- ifera and shells of ostracoids; and in this, as well as in its color and texture, it closely resembles the blue mud now in process of deposition in the deeper parts of the Gulf of St. Lawrence. It extends west to’ where the Laurentian ridge of the Thousand Islands crosses the St. Lawrence, and where the same rocks cross the Ottawa, and in gen- eral may be said to be limited to the Lower Silurian plain, and not to mount up the Laurentian and metamorphic hills bounding it. The Saxicava sand sometimes rests upon the Leda clay, sometimes upon Bowlder clay, and often on the older rocks. In some instances the surface of the Leda clay has been denuded and cut into deep trenches, and the sand rests abruptly upon it; in other cases there is a transition from one deposit to the other, the clay becoming sandy and eradually passing upward into pure sand. It must have been origin- ally a marginal and bank deposit, depending much for its distribution 42 Cincinnati Society of Natural History. on the movement of tides and currents. In some instances, as at Cote des Neiges, near Montreal, and on the terraces on the Lower St. Law- rence, it is obviously merely a shore sand and gravel, like that of the modern beach, | The terraces and inland sea cliffs have been formed by the same recession of the sea which produced the Saxicava sand. At Montreal, where the isolated mass of trap, flanked with Lower Silurian beds, constituting Mount Royal, forms a great tide-gauge for the recession of the Post-pliocene sea, there are four principal sea margins, with several others less distinctly marked. The lowest of these, at a level of 120 feet above the sea, corresponds, in general, with the level of the great plain of Leda clay in this part of Canada. On this terrace, in many places, the Saxicava sand forms the surface, and the Leda clay and Bowlder clay may be seen beneath it. Another at 220 feet in height furnishes Saxicava sand resting on Bowlder clay. Three other terraces occur at heights of 386, 440 and 470 feet, and the latter has, at one place, above the village of Cote des Neiges, a beach of sand and gravel, with Saxicava and other shells. Even on the top of the mountain, at a height of about 700 feet, large traveled Laurentian bowlders occur. | ~The prevalent Post-pliocene deposit on Prince Edward Island is a Bowlder clay, or in some places bowlder loam, composed of red sand- stones. Thisis filled with more or less rounded and striated bowlders of red sandstone, derived from the harder beds of the island. At Campbellton, however, in the western part of the island, a bed of Bowl- der clay is found filled with bowlders of metamorphic rocks, similar to those of the mainland of New Brunswick. Strise on the northeastern coast of the island have a direction S.W. and N.E. ; and on the south- western coast S. 70° E. | At Campbellton, in the sand and gravel above the Bowlder clay, Tellina greenlandica occurs, at an elevation of about 50 feet above the sea. On the surface of the country, there are numerous traveled bowlders. Those of granite, syenite, diorite, felsite, porphry, quartzite and coarse slates are identical, in mineral character, with those which occur in the metamorphic districts of Nova Scotia and New Brunswick, at distances from 50 to 200 miles to the south and southwest; though some of them may have been derived from Cape Breton on the East. Those of gneiss, hornblende schist, anorthosite and labradorite rock must have been derived from the Laurentian rocks of Labrador and Canada, distant 250 miles or more to the northward. Mesozoic and Cenozoic Geology and Paleontology. 43 In Nova Scotia and New Brunswick the Bowlder clay or unstratified drift varies from a stiff clay to loose sand, and its composition and color generally depend upon those of the underlying and neighboring rocks. Thus over sandstone it is arenaceous; over shales, argillaceous; and over conglomerates and hard slates, pebbly orshingly. The great- er part of the stones contained in the drift are, like the paste containing them, derived from the neighboring formations; though, in some in- stances, they have been transported from a distance. The transported bowlders have generally been drifted southward, though some have been carried northward, and others in different directions. They have especially been drifted from the more elevated and rocky districts to the lower grounds in their vicinity. The stris upon the rocks vary from north and south to east and west, though there is a general ten- dency to a southern and southeastern course. Alfred R. C, Selwyn* found many fine examples of ice-grooves and scratches on the rocky shores of Vancouver’s Island, where they occur in different directions, and sometimes nearly at right angles to each other. He quoted, with approval, the statement of Prof. J. D. Whitney, that northern drift does not occur in California, and that no evidence of its occurrence has yet been detected on the Pacific coast, as far north as British Columbia and Alaska. This conclusion having been arrived at on the authority of Mr. W. D. Dall, naturalist, attached to the Collin’s Overland Telegraph Company, and who states that though he had carefully examined the country over which he had passed, in Alaska, for glacial indications, he had not found any effects attributable to such agencies ; and that no bowlders, no scratches, or other marks of ice action had been observed by any of his party, though carefully sought for. And that inland, neither Mr. Selwyn nor his assistant Mr. Richardson observed any. That the superficial deposits of British Columbia are chiefly de- veloped in the ancieut terraces or benches, which, throughout the coun- try, are wonderfully regular and persistent, occuring from the coast up to elevations of nearly 4,000 feet, in the passes of the Rocky mountains. They give a marked and peculiar character to the scenery of the river valleys, rising like gigantic stairs, to elevations of sometimes more than four hundred feet above the adjoining river or lake. In some places - two, three, four and five distinct steps can be seen ; while often they have either become merged into one by subsequent denuding agencies, * Geo. Sur. of Canada. — 44 2 Cincinnati Society of Natural History. or-else the precipitous character of the side of the valley has altogether prevented their formation. The steps vary greatly’ in height, the greatest height observed being as much as one hundred feet ; in width, - from one to five chains is not uncommon. Nearly all the lakes in British Columbia occupy long, narrow de- pressions in the river valleys, and are, in fact, lake-like expansions of the rivers. There is no doubt that such lakes were at one time much more extended and more numerous than they now are; and that, in many places, as, for instance, at Lytton, and on the north bend of the Thompson, and at Canoe river crossing, the terraces mark the old margins of these lakes, while in others they doubtless represent only the ordinary flood-flats of the rivers. The removal of the rocky bar- riers by which these inland waters were confined would result in the formation of such gorges and canons as we now find on the Fraser at Gale, and below Lytton, as well as on the North Thompson at Murehi- son’s Rapids, and on Canoe river below the wide flats at the crossing, and would, without any general movement of elevation, drain off the waters of the lakes, leaving the old shore lines exactly as we now see them, at corresponding heights on both sides of the valleys. Ordinary alluvial river flats do not commonly occur in that manner, but where a flat occurs on one side there is usually a steep bank on the other, and especially is this so along rapid rivers which traverse a mountain- ous country. Dr. F. V. Hayden* said, that Fort Bridger is located in what appears to the eye a sort of basin, inclosed by high, arid table lands, but really in a central portion of the drainage of Black’s Fork. The beautiful valleys, Smith’s, Black’s, and Muddy, have been carved out of the horizontal strata, and between the streams are terraces and flat table lands, which give a singular outline to the surface of the country. No forces now in operation, in this vicinity, could have given the ex- isting features to the surface of the country, and the cause must have been local, proceeding from the northern slope of the Uintas. The beautiful table-top divides between the valleys, and streams are exten- sions into the plains of the radiating ridges of the mountain slope, and are literally paved, in many places, with the water-worn bowlders of the purplish sandstones and quartzites, and with the carbon- iferous limestones that compose the nucleus of the Uintarange. Here and there we can see a flat-topped butte cut off by erosion from some of the intervening ridges, and rising above the surrounding country as * U.S. Geo. Sur. of Wyoming. - Mesozoic and Cenozoic Geology and Paleontology. 45 a partial witness to the extent of the denudation. A little south ot west of Fort Bridger, is an isolated butte called Bridger’s Butte, which forms a prominent land mark to the traveler, and according to the barometer, rises 750 feet above the valley of Black’s Fork, at the fort. The summit appears perfectly level, and was estimated to be about two miles in length, from north to south, and about a fourth of a mile in width, from east to west. The upper portion of the butte is composed of the somber, brown, indurated, arenaceous clays, gray and rusty brown sandstones of the Bridger Group, passing down into limestones and marls of the Green river beds. In the brown clays are abund- ant remains of turtles, with a few fragments of other vertebrate re- mains. . at nya. belie ide ee alr ea sp nae 7 Pt , 7% Pas nh yes Pee M ee Tate RC NLR Oe : as ; ; - ys "N\ , . 4 - : >\ - > M 1 BANE , { E . ‘ e » a 7 ° « x 01 < . ed 3 i. ~ Ry = Geographical Distribution of Indigenous Plants. 55 direct line across the South Pole ; and with even a moderate amount of land intervening, it would not be very difficult for plants to find their way from one country to another, The similarity between the floras is abundantly illustrated by a table of fifty-five species of plants of temperate and cold South America, which represent the same num- ber of species in New Zealand and Australia. There are really 89 species, or nearly one eighth of the flora of New Zealand, which are also South American.* | The same explanation of the glacial epoch would account for the finding on the mountain of Kini-Balu, in Borneo, at 8,000 feet elevation, of three very peculiar Antarctic, Tasmanian and New Zealand genera, viz.: Drapetes, Phyilocladus, and Drimys, “which are almost unknown | in the northern hemisphere.” Having now shown that the long periods of time necessary for the wide distribution of plants are granted by the antiquity of the Ameri- can continent, and explained the importance of the glacial epoch to the theory, I shall now proceed to show the similarity existing between the floras of Europe and the northeastern United States, and show reasons for expecting this similarity. It has existed for a long time. In the Cretaceous rocks of Kansas and Nebraska, are found many plants of existing genera. The species of these genera are, many of them, closely allied to those now livingin America. When we turn to Europe, and compare our fossils with those of the Cretaceous forma- tions there, many of the species are found to be identical in both for- mations.{ Not only this, but we find in the Cretaceous rocks of Green- land, in 70 deg, N. latitude, the same fossil forms that formerly lived * Hooker Intro. Flor. New Zealand, pp. xxx-xxxvi. While on this subject, it might be well to state that Dr. Hooker found it difficult to account for the fact that though many typi- cal genera and species of New Zealand were found in Australia, only a few peculiar genera and species of Australia were found in New Zealand, though they were well adapted for transportation by ocean currents. The difficulty is partly solved when we find that the ocean currents run from New Zealand toward Australia, instead of in the reverse direction. Seeds could then only be transported from the former to the latter. Mr. Wallace, in his new book, on ‘‘ Island Life,’’ suggests another explanation. He supposes Australia to have been divided during the Cretaceous period into two islands, the Temperate on the west, and the Tropical on the east. -The eastern island was united to New Zealand by a spur of land, which allowed an interchange of fauna and flora, while the west island never was united to New Zealand. Finally, the channel which separated the east and westislands of Austra- lia was closed, and New Zealand and East Australia. were separated. If this explanation is the true one, then the greatest similarity should exist between East Australia and New Zealand; and the greatest difference be found between New Zealand and West Australia. This has been found to be the case, and the data can be found in Dr. Hooker’s essay, ‘** on the Flora of Australia,’’ 1859, pp. l-liv. + Hooker, Flora New Zealand, p. xxxvi. t See Lesquereux, Cretaceous Flora of the W. U.S. In U.S. Geo. and Geog. Sur. of Terr., W.ash., D.C., 1874, vol. vi. - 56 Cincinnati Society of Natural History. in temperate Europe and America. One of the most remarkable of these is a species of Sequoia. So similar are the fossils to the species now living in California, that there is no doubt but that they are the ancestors of our living trees. It may seem strange to some, to call to mind the fact that California is at present the only place where these _ trees now grow, when we know that they once flourished over a much more extensive area. But when wesee the peculiar character of the California climate, when contrasted with that of Europe, Eastern North -America, and Eastern Asia, at the present day, we are forced to the conclusion, that in their present situation only have they found the necessary requisites of their growth. It is to be feared that these re- markable forms of vegetation, connecting links between the past and the present, are now on the highroad to extinction; and in a few more decades they will be almost unknown in a wild state, and exist in history as another example of the destructive powers of mankind.* The species of plants which are, according to Gray’s Manual of Botany, common to Europe and Northeast United States,f can be divided into four classes. First, the strictly Alpine species, found mostly on the highest summits of the White mountains, the Adiron- dacks, and in other elevated localities. The distribution of all these species, I believe to have been effected by means of the glacial period, as already explained (ante p. 54). The species are as follows : List No. I.—Strictly Alpine species, all having a north or north- westward range. / 1. Cardamine bellidifolia. ; 18. Castilleia pallida. 2. Viola palustris. 19. Euphrasia officinalis. 3. Silene acaulis. 20, Diapensia lapponica. 4, Sibbaldia procumbens. 21. Polygonum viviperum. 5. Potentilla frigida. | 22. Oxyria digyna. 6. Saxifraga rivularis. 23. Empetrum nigrum. 7. Saxifraga stellaris, var. comosa. | 24. Salix herbacea. 8. Epilobium alpinum. 25. Luzula arcuta. 9. Epilobium alpinum var. majus. 26. Luzula spicata. 10. Gnaphalium supinum. 27. Juncus trifidus. 11. Vaccinium uliginosum. 28: Scirpus czespitosus. 12. Arctostaphylos alpina. 29, Carex scirpoidea. 13. Cassiope hypnoides. 30. Carex capitata. 14. Bryanthus (Phyllodoce) taxifo-| 31. Carex vitilis. lius. 32. Carex rigida. 15. Rhododendron lapponicum. 33. Carex atrata. 16. Loiseluiria procumbens. . 34. Phleum alpinum. 17. Veronica alpina. 35. Agrostis Canina. * Address by Prof. A. Gray, before Am. As. Adv. of Science, 1872. Reprinted in Darwin- jana, p. 200. . + All States north of Tennessee and North Carolina, and east of the Mississippi river. + Pen we / | Geographical Distribution of Indigenous Plants. 57 36. Poa laxa. 37. Festuca ovina. 38. Triticum violaceum. 39. Aira atropurpurea. 40. Hierochloa alpina. These forty species comprise all those found in our Alpine region ; and there are but nine species found here, which are not also found in Kurope. These are as follows : Nabalus nanus. Vaccinium czspitosum. Salix cutleri. . Calamagrostis pickeringii. e Arenaria greenlandie¢a. Geum radiatum, var. Peckii. Solidago thrysoidea. Arnica mollis. Nabalus boottii. The first, though not occurring in Europe, is an Alpine and Arctic form, and has been found in Greenland. Gewm radiatum is a native of the high mountains of Carolina, and the variety only is a northern Alpine form.* Solidago thrysoidea, is very near European form of S. Virg-aureat (also found in America), and may be a geographical variety. Vaccinium cespitosum is found in Labra- dor, and as far north as Alaska. The few remaining may be forms which have been developed from others, on account of the struggle for existence which ensued when left on the mountains during their re- turn to the north at the close of the glacial epoch. The, second list consists of sub-Alpine and other species, having a north or northwestward range ; and the distribution of these admits of the same explanation as No. I. List No. IL. — Sub-Alpine and other species, having a north or northwestward range. Anemone nemorosa. Anemone (Hepatica) triloba. Ranunculus repens. Coptis trifoliata. Acta spicata, var. rubra. Cardamine pratensis. Arabis petra. Arabis hirsuta. Arabis perfoliata. _ Barbarea vulgaris. Erysimum cheiranthoides. Draba incana. Draba nemorosa. Viola selkirkii. Viola canina, var. sylvestris. Arenaria lateriflora. Arenaria peploides Stellaria longifolia. Stellaria longipes. - Stellaria borealis. Stellaria humifusa. * Gray’s Manual, p. 153. Cerastium arvense. Sagina nodosa. Lepigonum (Spergularia) rubrum. Lepigonum salinum. Lepigonum medium. Hypericum mutilum. Geranium robertianum. Oxalis acetosella. Astragalus alpinus. Oxytropis campestris. Vicia cracea. Lathyrus maritimus. Lathyrus palustris. Spirzea salcifolia. Spireea aruncus. Agrimonia eupatoria. Dryas integrifolia. Geum macrophyllum. ‘Geum strictum. Geum rivale. Potentilla Norvegica. + Ibid, p. 241. \ 58 ‘Cincinnati Society of Natural History. Potentilla anserina. Potentilla fruticosa. Potentilla palustris. Fragaria vesca. Rubus chamzmorus. Ribes rubrum. Saxifraga oppositifolia. Saxifraga aizoides. Saxifraga tricuspidata. Saxifraga aizoon. Sedum rhodiola. Circea alpina. Epilobium augustifolium. Epilobium palustre, var. lineare. Linnea borealis. Lonicera cerulea. Viburnum opulus. _ Galium aparine. Galium trifidum. Galium boreale. Erigeron acre. Solidago virga-aurea. Achillea millefolium. Artemisia borealis. Artemisia canadensis. Gnaphalium uliginosum. Senecio palustris. Taraxacum dens-leonis. Lobelia dortmanna. Campanula rotundifolia. Vaccinium vitis-idzea. Vaccinium oxycoccus. - Aretos taphylos uva-ursi. Andromeda polifolia. Cassandra calyculata. Calluna vulgaris. Chimaphila umbellata. Moneses uniflora. Pyrola secunda. Pyrola rotundifolia. Monotropa hypopitys. Primula farinosa. Primula mistassinica. Lysimachia thyrsiflora. Glaux maritima. Gentiana (detonsa) serrata. Pleurogyne carinthiaca, var. pusilla. Menyanthes trifoliata. Polemonium ceruleum. Mertensia maritima. Convolvulus sepium. Veronica scutellata. Veronica ser pyllifolia.. Rhinanthus crista-galli. Pinguicula vulgaris. Calamintha clinopodium. Scutellaria galericulata. Brunella vulgaris. Stachys palustris. Chenopodium (Blitum) rubrum. Chenopodium (Blitum) capitatum. Atriplex patula. Coriospermum hyssopifolium. Polygonum lapathifolium. Polygonum hydropiper. Polygonum amphibium. Polygonum aviculare. é Rumex longifolius. Humulus lupulus. Myrica gale. Beluta alba, var. populifolia. Alnus viridis. Alnus incana. Salix myrtilloides. Juniperus communis. Juniperus communis, var. alpina. Juniperus sabina, var. procumbens. Taxus baccata, var. canadensis. Calla palustris. ‘ Sparganium simplex. Sparganium minimum. Scheuchzeria palustris. Habenaria viridis, var. bractrata. Habenaria hyperborea. Habenaria obtusata. Goodyera repens. Spiranthes romanzoviana. Listera cordata. Calypso borealis. Microstylis monophyllos. Liparis loeselii. Corallorhiza innata. Tofieldia palustris. Streptopus amplexifolius. Smilacina stellata. Smilacina bifolia. Alliam schceenprasum. Narthecium ossifragum, var. ameri- canum. Luzula pilosa. Luzula parviflora, var. melanocarpa. Luzula campestris. Juncus filiformis. Juncus balticus. Juncus stygius. Juncus bufonis. Juncus gerardi. Juncus alpinus, var. insignis. 4 Cyperus flavescens. . Scirpus pauciflorus. Eriophorum alpinum. Eriophorum vaginatum. Eriophorum polystachyon. Eriophorum gracile. Carex pauciflora, Carex disticha. Geographical Distribution of Indigenous Plants. 59 Carex teretiuscula. Carex teretiuscula, var. major. Carex chordorhiza. Carex tenuiflora. Carex stellulata. Carex tenella. Carex vulgaris. Carex aquitilis. Carex limosa. ‘Carex irrigua. Carex alpina. Carex livida. Carex panicea. Carex panicea, var. refracta. Carex pallescens. Carex capillaris. Carex flava. Carex viridula. Carex filiformis. Carex aristata. Carex pseudo-cyperus. Carex miliaris. Carex rariflora. Agrostis vulgaris. Agrostis alba. Cinna arundinacea, var. pendula. Calamagrostis stricta. | Calamagrostis langsdorffi. Calamagrostis lapponicum. Calamagrostis arenaria. Keeleria cristata. Poa annua. Poa compressa. Poa alpina. Poa cesia. Poa serotina. Poa pratensis. Triticum repens. Triticum caninum. Elymus sibericus. Aira ceespitosa. Aira flexuosa. Hierochloa borealis. Triticum subspicatum, var. molle. Phalaris arundinacea. Millium effusum. The distribution of some of these requires a little explanation. Of the following none are known to pass to the north of latitude 50 deg. in this country, though they are found as far north as 70 deg. in Europe. Ranunculus repens. ~ Oxalis acetosella. Vicia cracca. Geum rivale. Geum strictum. Geranium robertianum. Veronica officinalis. Atriplex patula. Juncus stygius. Cyperus flavescens. Microstylis monophyllos. Humulus lupulus. Millium effusum. This apparently anomalous distribution will be explained when we find that the isothermal line of 40 deg. Fahr. passes a little to the south of latitude 50 deg. in North America, and a little to the south of latitude 70 deg. in Europe. It may, therefore, well be that the temperature of this country is not now high enough to allow these plants to pass the 50th deg ; and it is reasonable to suppose that when it was milder the species lived as far north as in Europe. The true Betula alba extends into the Arctic regions in Europe. Our representative of the species, the variety populifolia, is not found . north of latitude 46 deg. We may, therefore, say that our variety is a southern form, the ancestor of which, at a former period of time, lived in the far north, but owing to an increase of cold it has become ex- tinct, leaving the variety as its southern representative. So, too, with Taxus baccata, var. canadensis. Our variety is probably the 60 Cincinnati Society of Natural History. southern representative of the European fourm. This variety does not extend further north than latitude 50 deg. on the eastern side of the continent, and “there are yew trees with the port of the ordinary 7. baccata in Oregon.”* Spiranthes romanzoviana has a peculiar distribution, and though found in this country, from New York to Lake Superior, and north- westward, it is known in Europe in but one place, viz : at Bantry bay, on the west coast of Ireland.+ May it not be a waif on the European continent, perhaps carried by birds or the Gulf stream across the ocean? Or is it a remnant of a once more widely distributed species, now confined to a single locality in Europe, but widely distributed in America ? List No. IfLI.—Consisting of species living either entirely in the water, or else in swamps, marshes and wet places. Those ranging north of latitude 50° marked “ N.”’ Ranunculus aquatilus, var. stagna- lis (N). Ranunculus aquatilus, var. tricho- phyllus (N). Ranunculus flammula, var. reptans (N). Ranunculus sceleratus (N). Caltha palustris (N). Nuphar luteum. Nuphar luteum, var. pumilum (N). Nasturtium palustre (N). Cardamine hirsuta (N). Drosera rotundifolia (N). Drosera longifolia. Stellaria uliginosa (N). Stellaria crassifolia (N). Myriophyllum spicatum (N). Myriopbyllum verticillatum. Hippurus vulgaris (N). Ludwigia palustris (N). Ligusticum scoticum (N). Sium angustifolium (N). Bidens cernua (N). Statice limonium (N). Statice limonium, var. caroliniana (N). Samolus valerandi, var. americana. * Utricularia vulgaris (N). Utricularia minor (N). Utricularia intermedia (N). Limnosella aquatica, var. tenuifolia (N). Veronica anagallis (N). Salicornia her bacea (N). Suzeda maritima (N). Ceratophyllum demersum (N). Callithriche verna (N). Callithriche autumnalis (N). Speirodela (Lemna) polyrrhiza (N). Lemna triscula (N). Lemna minor (N). Typha angustifolia. Typha latifolia (N). Sparganium simplex, var. angusti- folium (N). Sparganium simplex, var. fluitans N). : Naias major. Naias flexilis. Zannichellia palustris. Ruppia maritima. Potamogeten natans (N). Potamogeten rufescens (N). Potamogeten gramineus (N). Potamegeten lucens (N). Potamogeten prelongus (N). Potamogeten perfoliatus (N). Potamogeien obtusifolius. Potamogeten crispus (N). Potamogeten compressus. Potamogeten pusillus (N). Potamogeten pusillus,var. major(N). Potamogeten pusillus, var. vulgaris. Potamogeten pectinatus (N). Triglochin palustre (N). Triglochin, maritimum (N). * Gray, Am. Jour. Sci., 2d series, vol. xxili., p. 67. + Gray’s Manual, p. 505. ¥ Geographical Distribution of Indigenous Plants. 61 Alisma plantago, var. americana | Carex maritima (N). ) Carex canescens (N). ' Vallisneria spiralis. Carex buxbaumii (N). Juncus effusus (N). Carex fulva. Juncus auriculatus (N). Carex extensa. Eriocaulon septangulare (N). Carex riparia (N). Eleocharis palustris (N). Carex paludosa. Eleocharis acicularis (N). ; Leersia oryzoides (N). Scirpus pungens (N). Alopecurus aristulatus (N). Scirpus supinus, var. hallii. Spartina juncea. Scirpus maritimus (N). Spartina stricta. Scirpus sylvaticus (N). Glyceria fluitans (N). Rhyncospora alba (N). Glyceria maritima (N). Carex gynocrates (N). Glyceria distans(N). Carex norvegica (N). Phragmites communis (N). Carex salina (N). The plants of this list, as noted at its head, alllive either entirely in the water, or else in swamps, marshes or wet places. We know that for some reason or other, all forms of life inhabiting the water, are more cosmopolitan. than terrestrial forms. Fishes, aquatic reptiles, fresh- water shells, water mammals, and wading or swimming birds, are all more generally distributed over the world than terrestrial species of the same classes. So, too, it is with plants. These have many facili- ties for migration, which other forms of life have not. Not least among them is the chance of their being carried in the mud, adher- ing to the legs, feet, and bills of aquatic and wading birds,* which often range over extensive tracts of country. The water communica- tion existing between the northwest coast of America, and the valley of the Mississippi, forms a natural highway for the migration of aquatic plants. The Yukon, the Mackenzie and its tributaries, the Red river of the North, the Mississippi and its tributaries, the Great Lakes and the St. Lawrence, form an almost uninterrupted water-way from Asia to the United States, and it can not be considered remarkable that 63 out of these 89 water plants have a northern extension, at least as far north as 90 deg. latitude. Of the remaining 23, some special re- marks must be made. Nuphar lutewm, the first on the list not found north of latitude 50 degrees, has been found but once in America. “ The only specimen seen like European “form,” says Gray, “was from Manayunk, seven miles below Philadelphia.”+ Now,as the variety pumdlum, also a- native of Europe, has a northern extension, it is probable that the single specimen may have been introduced in some way, especially as it was found soclosetoa largecity. Carex norvegica has also been found * See Darwin, Origin Species, 6th ed., p. 328. + Gray’s Manual, p. 57. a \ . = 62 Cincinnati Society of Natural History. s in but one place in this country, viz: at Wells, Maine, in a salt marsh.* Carex fulva has been found but once (at Tewksbury, Mass.) in the United States,t though it grows in Newfoundland, and is scarcely known ~ - north of latitude 60 deg. in Europe.t Carex extensa has also been found in but one locality in America, viz: on the coast of Long Island, on the border of a salt marsh.§ Carex paludosa is only known from the border ofa salt marsh at Dorchester, Massachusetts, and is per- haps naturalized from Europe. We have here, then, five species which are confined to one locality each, and all have been found under such circumstances as to justify the belief that they have been introduced by some agency, since the advent of man in America, and are not properly native. Drosera longifolia does not grow north of latitude 47 deg. in America ; but as it has not been found in Lapland, we may assume this to be a casein which the species is not capable of living now in high latitudes, though it may have done so when the climate was milder. This is the case, also, with the following, none of them growing to the north of 48 deg. latitude in America, nor of 55 deg. in Europe. 4 Myriophyllum verticillatum. Naias flexilis Zannichellia palustris. Ruppia maritima. Vallisneria spiralis. Potamogeten compressus. Typha angustifolia. Potamogeten obtusifolius (?). -Naias major. Carex riparia. Samolus valerandi, of Europe, is represented in America by the variety americana ; and as this does not extend north of latitude 50 deg. in United States, nor the species above 55 deg. in Europe,** we may understand that the variety flourishes here as the representa- tive of the other form. With Potamogeten pusillus, var. vulgaris, ‘though the species grows in high latitudes in both Europe and America, the variety does not. The variety halli, of Scirpus supinus, is the eastern form, produced probably by climatic or other changes, for the true form is found in Texas.tt The two remaining species, Spartina juncea, and S. stricta are both found in salt marshes, or on sea beaches. Gray says: ‘‘ The two species of Spartina belong proper- * Gray’s Manual, p. 578. + Ibid, p. 594. t Gray, Am. Jour. Sci., 2dseries, vol. xxiii., p.67. Watson in Geog. Dist. Plants, p. 252, says 55° instead of 60°. § Gray’s Manual, p. 594. || Ibid, p. 596. { See Watson, Geog. Dist. of Brit. Plants, Appendix II. Also, Gray, Am. Jour. Sci., vol. xxiili., pp. 67, 68. -* Wiatson, UaresmeDeicoos t+ Gray’s Manual, p. 563. : ; Geographical Distribution of Indigenous Plants. 63 | ly to America, being found in only a few places on the coast of Europe, where they seem to have effected a chance lodgment.’’* The next list, No. IV., includes all the plants, as far as known, com- mon to Europe and the Northeast United States, not enumerated:in the three preceding tion. The list is as follows: and nearly all of them require some special observa- List No. LV. Myosurus minimus. Cardamine hirsuta, var. sylvatica. Draba verna. Subualaria aquatica. Sagina apatela. Sagina procumbens. Lepigonum medium, var. melano- carpa. . Oxalis corniculata, var. stricta. Potentilla argentea. Circzea lutetiana. Lythrum hyssopifolium. Centunculus minimus. Scrophularia nodosa. Salicornia virginica. Salicornia frutivosa, var. ambigua. Salsola kali. Polygonum erectum. Polygonum dumetorum, var. scan- dens. Rumex maritimus Castanea vesca, var. americana. Convallaria majalis. Cyperus rotundus, var. hydra. Carex muricata. Carex limula. Carex levigata. Hordeum pratense. Myosotis arvensis. Taking the first on the list, Myosurus minimus, we find it has a scattered distribution. Found from Illinois to Kentucky, thence south and west;+ Florida and Georgia. It is given in catalogues of Plants of Indiana,§ of Iowal| (at Davenport), and in Kansas.4]_ It also grows in Oregon, along with the only other species, M@. aristatus, which is also foundin Chili.** In Europe, it does not extend north of latitude 55 deg.tt Prof. Gray considers that it may have been introduced in our district,{{ and even if not it may be considered as coming under those species referred to in List No. II., as not able to live at the north now, though it may have done so when the climate was milder. | Draba verna grows in “sandy waste places and road sides. Not found north of Lower Canada,’’§§ and perhaps not so far north, for it is not given in catalogues of Plants of Buffalo nor Chautauqua, N. Y., * Gray, Am. Jour. l.'c., p. 66. + Gray’s Manual, p. 44. + Am.:Jour. J; .¢., vol. xxili., p. 381. 2 Bot. Gazette, Feb., 1881. || Arthur’s Catalogue. { Carruth’s Catalogue. ** Am. Jour., vol. xxiii., p. 382. tt Watson, lJ. c., p. 187. tt Proceed. Am. Ass. Ady. Sci., 1872, appendix. 22 Gray’s Manual, p. 72. 64 Cincinnati Society of Natural History. Michigan, Wisconsin, Iowa, nor Kansas. Gray considers it to have been introduced by man. In Europe it is said not to occur north of latitude 55 deg. Potentilla argentea is in the same category. It is not known to pass north of latitude 50 deg. in America, although it reaches to 70 deg. in Europe. Myosotis arvensis “is not common here, and has probably been introduced.”’* In Europe, it is found as high as 70 deg. latitude.t . Subularia aquatica is a rare plant in North America, having been . found only in Maine and New Hampshire.t “From its size, aspect and place of growth, it is exceedingly liable to be overlooked” (Gray). In Europe, it is found as far north as 72 deg. latitude.§ Sagina apa- tella is found in “ Dry soil, N. Y., and Penn. to Ill., scarce, seemingly native.” || It is not given in catalogues of plants of Buffalo, Chautau- qua, Dist. Columbia, Michigan, Ohio, Iowa, Kansas, Wisconsin, nor Canada. It must be, therefore, either very scarce or easily over- looked, and has most likely been introduced in some few places. It does not extend further north than latitude 55 deg. in Europe. The following ten species are all found in this country, at least as far north as latitude 50 deg., and none of them extend north of lati- tude 55 deg. in Europe. Their distribution is explained under the rule already laid down in regard to some species of List No. II. (ante p. 59), only in this case they stop at 55 deg. in Europe, instead of extend- ing to 70 deg. as do the former ones. : Sagina procumbens. Centunculus minimus. Circza lutetiana. Rumex maritimus. Scrophularia nodosa. | Carex muricata. Salsola kali. Carex levigata. Lythrum hyssopifolium. Hordeum pratense. Of the following all are varieties of European species. Sometimes the species and variety are both found here, and sometimes the latter a only. In the former case, it is found that the variety is the more com- — mon to the southward, if not wholly confined there. In the latter case, we may consider that we have here cases in which the species has varied to a certain degree in the south and been maintained there, while the parent species has ceased to live at the north on account of the cold. These species are as follows : * Gray, Am. Jour.,/. c., p. 65. + Watson, J. c., p. 65. t Gray’s Manual, p. 73. 2 Watson, l.c., p. 191. || Gray’s Man., p. 94. { Watson, l. c., p. 195. K 33 Geographical Distribution of Indigenous Plants. 65 Cardamine hirsuta, var. sylvatica. Polygonum dumetorum, var. scan- Lepigonum medium, var. macrocar- dens. : a. Castanea vesca, var. americana. Oxalis corniculata, var. stricta. Cyperus rotunda var. hydra. Salicornia fruticosa, var. ambigua. There remains now of list No. IV. but four species. Of these Salicornia virginica has been rather doubtfully identified with S. mucronata of the coast of Spain. Polygonum erectum, a very common plant around all houses, has doubtless been introduced by man, Carex limula has been rather doubtfully identified with the Lapland plant, by Wm. Boott.* There then remains only Convallaria majalis. This is known to grow in this country only on the mountains of Georgia and North Carolina, “ and extends north to the peaks of Otter, in Virginia, latitude 374 deg., at an altitude of 4,000 feet ; but it is not known to occur anywhere beyond this; while in western Europe it extends nearly to latitude 70deg.”’; This certainly is aremarkable case, and is difficult to account for. It is hardly possible it has been overlooked, for it is too striking a plant. I have a specimen, collected in Massa- chusetts, escaped from cultivation, and it is given in the catalogue of Plants of Wisconsin. It seems to be in much the same position on the Atlantic coast, as Sequota is on the Pacific ; now confined to limited localities, though once ranging over wide tracts of country. Enumerated in the four preceding lists, there are 360 species and varieties of plants. A reasonable explanation of why they are found in both Europe and America has been given. But as a foundation for — the explanation, two things must be admitted. First, that the region surrounding the North Pole has been the source from which has been - derived a good part of the floras of Europe, North America, and Asia ; and, second, the occurrence of glacial and inter-glacial (warm) periods both north and south. | As for the first, the region close around the North Pole is, as yet, a terra incognita. We know enough of it, however, to say with cer- tainty that there is considerable land clustered in its vicinity. We may very reasonably suppose, that during the warm period at the North, the ocean was ata lower level than it is now,{ and that a land con- nection formerly existed between the northwest coast of America, and * Gray’s Manual, p. 582. 7 Am. Jour. l. c., vol. xxiii., p. 64. ‘t In consequence of the withdrawal of large quantities of water to form the Antarctic ice cap; and because the shifting of the earth’s cénter of gravity caused by this ice, would have a tendency to draw the water toward the south, thus leaving much dry land at the north. Croll, ‘* Climate and Time.’’ 66 — Cincinnati Society of Natural History. the northeast coast of Asia.* With this connection the facilities for migration would be greater, and would be decidedly taken advantage of by animals and plants. There is also the same reason for supposing that, during that period, the stretch of ocean between Greenland, Iceland, and the northwest of Europe, was much less than it is now, even if the continents were not actually united. We know, further,t that at a former period of time, the climate there was such as to admit of the growth of plants, which are now strictly confined to temperate regions; and which certainly could not grow under the climatic con- ‘ditions existing at the present day in the countries under the Arctic circle. | The resemblance between the floras of Europe and the United States, is by no means confined to the 360 identical species. There are, be- sides, many closely related species, some of which may be reduced to geographical varieties; and a still larger number of strictly represen - tative species, not likely to be confounded.{ If to the identical species we add these related and representative species, we shall find that one third of the 2,277 indigenous species given in Gray’s Manual, resemble European forms. But the similarity between the floras of North - America and Europe, is by no means confined to the small territory with which I have been dealing. I selected the portion ¢govered by Gray's Manual, because the country has been more thoroughly ex-. plored, and because the facilities for getting imformation are better than for other and larger tracts of country. It is well known that | many European forms extend along the Rocky Mountains to Colora- do, and other elevated localities, and I Have no doubt but that a com- parison of the entire flora of the United States (excluding the semi- tropical one of California, which really belongs to the Mexican region), will show nearly as much resemblance as I have shown exists in the small territory here dealt with. As for the glacial period and its effects upon the country, few are now inclined to deny it; and they grant not only the occurrence of cold periods but of warm ones intervening. Undoubtedly we may look to the north for the place of origin of many of our species of plants; . and in the glacial theory will find the principal factor for the disper- sion of the species “oo the place of their origination. ' * A rise of less than 200 feet would ae this connection. Croll estimates that the fall of the level of the ocean in consequence of the withdrawal of water, was some 600 or 800 feet at Edinburgh, and would be more further toward the north. + By the discovery of fossil plants at Disco, Greenland, and other places, and by the abundant coal fields of high northern latitudes. t For some of these species, see Am. Jour. Sci., /. ¢., vol. xxiii., pp. 80-85. \ } | \ a ’ { ‘ iN =) yr epi \ ' ia iB Geographical Distribution of Indigenous Plants. 67 Prof. Gray has made it well known that there is far more resem- _ blance between the plants of the Atlantic coast of the United States, and the Pacific coast of Asia, than between the latter and the Pacific coast of America, especially of California. But this can not be con- sidered so very remarkable when we come to note the very marked dif- ference in the climate between the two sides of the continent. The Eastern and the Asiatic climates resemble each other very much more than the Californian. In the first two we have four well marked sea- sons, characterized by abundance of moisture, while in California there are but two, the wet and the dry, as in tropical countries. The dry season is So severe as to cause the death of all plants for whose growth continual moisture is necessary; and we find that the majority of plants common to eastern North America and western Asia, but absent from California, are among the very ones for whose growth, moisture, and especially shade, isnecessary. Of the latter, many parts of California are utterly destitute. In reality we have, in California, a continuation of the climatic conditions existing in Mexico and the semi-tropical parts of America; and not only is the flora closely allied to that of Mexico, but the fauna also. It forms a separate region in Wallace’s “ Distribution of Animals,” and must, in any general classification, be separated from the rest of America, because of many peculiarities. We have, therefore, many good reasons for not finding there more than 76 species out of 258 living in America and Asia. To sum up our observations, then, we find: lst. That the time necessary for the distribution of our plants has been sufficiently long. 2d. That the species of plants common to Europe and America have had a common origin in the land about the North Pole. 3d. That they have migrated south on account of the cold in the Arctic regions. Ath. That on account of present climatic conditions, some species reaching a high latitude in Europe are not found in America as far north by 20 deg. 5th. That the chain of the Rocky mountains, and the Andes, fur- nishes, or has furnished, a highway for the dispersion of some Arctic forms over the southern hemisphere. And 6th. That the similarity between the floras of Europe, of Northeast Asia, and Eastern America, is greater than that between Asia and the American Pacific coast, on account of the great difference in cli- matic conditions, and because of the closer connection which exists be- tween California and the semi-tropical region of Mexico. — 68 Cincinnati Society of Natural History. DESCRIPTION OF THE YOUNG OF THE GRIZZLY BEAR —URSUS HORRIBILIS. By CuHaries Dory. Plate III., natural size; three days old. The fine pair of grizzly bears, presented to the Zoological garden by Mr. J. J. Bantlin, have, for the third time, brought forth young. The adults are now eight years old. The first cubs were born J anuary, 1876, and immediately eaten up by their mother. January, 1878, two more were born, and were overlaid, after living three days. They measured 102 and 114 inches respectively, from the tip of the nose to the end of the tail ; eyes, tightly closed. On Janu- ary 10, 1881, the female was delivered of the last, a litter of three. Through the kindness of Mr. Frank J. Thompson, superintendent of the garden, I have been permitted to examine these most interesting specimens and to secure the following data in regard to them. Mr. Thompson informs me that the period of gestation is within a day vr two of nine months, he having carefully observed their actions while he has been in the garden. At first sight, one is impressed with the very small size of the cubs in proportion to the great size of the parents. Shortly after the birth of the third cub, the mother came away from them, and it was decided to remove them and try to rear them by hand. When brought away, and warmly wrapped in Angola goat skin, the little creatures sucked readily from a bottle filled with cow’s milk. They were very strong and vigorous, and when chilled or handled, manifested their displeasure with vociferous yells, that in tone resembled the cries of a very young human infant. Measurements and weights were as follows : Ist. Length from tip of nose to end of tail, 94 inches; circumference of body, behind fore leg, 84 inches; length of foreleg, from head of humerus to claw, 34 inches; claw of forepaw, 5-l6ths inch; girth of head, 52 inches; length of head, 24 inches; weight, 1 Ib. 34 oz. 2d. Length, from tip of nose to end of tail, 104 inches; girth, 8 inches; foreleg, 34 inches; weight, 1 lb. 24 oz. 3d. Teneth, 94 inches;. girth, 74 inches; weight, 1 lb. 2 oz. Color.—The body was of a dusky flesh tint, thickly covered with short, stiff hair, of a dirty white color, with a broad dorsal line of ash colored hairs, from the occiput to the tail. The face was rich flesh color. The nose reddish pink, as were also the ears. The soles of the feet were bright carmine pink, Eyes, tightly closed. The subject of the illustration was 3.days old. ~ t { _ Description of Some New and Remarkable Crinoids. 69 | - DESCRIPTION OF SOME NEW AND REMARKABLE | CRINOIDS AND OTHER FOSSILS OF THE HUDSON RIVER GROUP, AND NOTICE OF STROTOCRINUS BLOOMFIELDENSIS. By S. A. MILuer, Esq. PALAASTER EXCULPTUS, 0. Sp. Plate I., fig. 1, natural size. Pentagonal ; rays a little longer than the diameter of the body ; diameter of the body about 93-100 inch ; length of ray measuring to the center of the body or disc, about 14 inches; breadth of a ray at the junction with the body, about 57-100 inch; rays obtusely pointed. The marginal range consists of somewhat quadrangular plates, hav- ing a width a little greater than the length; the first eight of these . have a length of } inch, and there are about eighteen in the length of, an inch, and not far from twenty-five in each range, though the speci- men does not permit us to make the count with certainty. The sur- face is strongly tubercular, and was probably spinous. a ~The adambulacral range consists of about twenty-eight plates, on a each side of a ray; they are narrower than the marginal plates, but :! have about the same length. Each plate bore strong spines, and some © of them, preserved on our specimen, have a length greater than the length of a plate. A single, somewhat pentagonal or irregular axillary plate, rests between the terminal marginal plates and the angle formed by the junction of the adambulacral plates. The extension of the wedge-shaped marginal plates into this angle is by gaping, and the axillary plate seems to fill this gape and to rest upon the extension of the marginal plates, supported by four adambulacral. plates, which abut against it. The ambulacral plates have their greatest length across the rays, thus providing a wide ambulacral furrow. Each plate is furnished with a sharp ridge in the middle, that curves slightly outward, from the center toward the adambulacral range, increasing in height, until it approaches or abuts against the adambulacral plate. The plates have a length in the direction of the rays one half greater than in P. granulosus, the ridge is higher and stronger, and occupies the central part of the plate, instead of commencing at the outer posterior angle, and terminating on the anterior inner angle of one plate, and re- 4 versing this direction on the next adjoining plate, as in P. granulosus. _. The character of these plates alone will, therefore, serve to distinguish 70 Cincinnati Society of Natural History. — this species from P. granulosus, and other species having about the same size and general outline. The appearance of having been carved out, which is presented by the ambulacral plates, suggested the specific name, The dorsal side and madreporiform tubercle unknown. This species is founded upon a single specimen, from the upper part — of the Hudson River Group, near Waynesville, Ohio, and is from the collection of I, H. Harris, Esq., of that place. CYCLOCYSTGIDES MAGNUS. Plate I., fig. 2, natural size; fig. 2a, magnified two diameters. Cyclocystoides magnus, Miller and Dyer, 1878, Jour. or Cin. Soc. or Nat. Hist., vol. i., p. po. pl. Ti. fics’ 8, Sa. The specimen of this species now before me has been worn upon the surface, and much of the plates composing the ring has been rubbed off, and three of the plates have been entirely removed; but, otherwise, étis much better than any I had seen, at the time, of establishing the species; indeed, it is the only specimen in this genus, that [ have ever seen, from which one could gather any idea of the central part of the disc or body. In comparing the original illustration with that now given, one must bear in mind, that the inner part of the rim of the specimen now illustrated has been worn down to the level of the outer rim, and the scars or mammillary elevations are scarcely discernible, though enough can be detected to show the double character of the plates forming the ring, and to leave no doubt of the correctness of the specific identification. The ring that surrounds the disc is composed of twenty plates, arranged, with reference to their length and connection with the central part, into ten pairs. Two of the shorter plates, each having two radiating channels toward the central part of the disc, are followed by two ofthe longer plates, each of which is possessed of three radiating - channels. This arrangement furnishes fifty channels connecting the ring with the radiate system of the disc; but the two chan- nels from one of the shorter plates, unite with the three channels of the adjoining longer plate, before reaching the central part of the disc, and, at this part of the disc, the channels are, therefore, reduced to ten. The central part of the disc of our specimen is too much in- jured for us to follow this system nearer to the center. The injury is apparent in fig. 2, but in the magnified view, fig. 2a, the injury is patched up by the erroneous substitution of plates. Whether, there- fore, the central part of the disc was connected with the ring by ten channels, which increased, by bifurcation, as they approached the ring Description of Some New and Remarkable Crinoids. 71 ee of fifty, or whether the ten channels were reduced to five before they united at the center, as seems quite probable, we are unable to deter- mine. The whole disc within the ring was covered with plates that seem to have imbricated toward the center, and the condition of | the preservation of our specimen is such that the series of radiating channels appear to have inosculated, but whether this appearance has resulted from the erosion of part of the imbricating plates, or really _ represents the true character of the radiating circulation of the animal, is not fully determined. : It would seem probable, from what we know of this species, that it consisted of a central disc, which was covered by numerous small plates and surrounded by a rim composed of twenty-plates, which bore upon its outer surface another rim or border having as many or more scars, or mammillary elevations upon it, as there were circulating channels connecting it with the disc. That from the central part of the disc, there arose either five or ten radiating channels, which bifurcated and possibly inosculated and pierced the rim in fifty places. That the cir- culation passed through the rim into the outer border. That the scars upon the outer border represent the cicatrices of ossicula. That there was a circular circulation through the rim, and as the rim is tuber- culous, there may have been a porous connection with the outer world through it. The specimen illustrated is from the collection of {. H. Harris, Esq., of Waynesville, Ohio, and was found in the upper part of the Hudson River Group, in that locality. a XENOCRINUS, N. gen. [Ety.—Xenos, strange, new; krinon, a lily.] Body, proportionally, rather long and gently expanding, so that its diameter, at the free arms, is only one half or two thirds of its length. Basals, four; no subradials; primary radials three; secondary radials four, five, six, or more, which enter into and form part of the cup or body; interradial and inter-secondary radial areas deeply excavated and filled by numerous small plates; azygous interradial area contain- ing a vertical: series of plates, to the top of the body, of about the same size as the radial plates, which rest upon a basal plate and occupy the central part of the azygous area, and between which and the primary and secondary radials, on either side, there is an excavated area filled by numerous small plates, as in the four regular interradial areas. ‘The vertical series, however, continues to the top of the pro- boscis, which is prolonged to or beyond the extension of the arms. ‘\ 72 Cincinnati Society of Natural History. | Arms, ten; pinnule, long, quite in contact, and some of the lower ones appearing to become incorporated into.the body or cup; column, quadrangular. ; XENOCRINUS PENICILLUS, Nl. Sp. Plate I., fig. 3, natural size, showing azygous side; fig. 3a, same specimen magnified two diameters; fig. 3b, magnified view of the azygous side of a compressed specimen; fig. 3c, view _ a the posterior side of a specimen, showing the arms and pinnulx, magnified about half its iameter. Basals.—Basals, four, uniting at the angles of the column, about twice as wide as high, two of them are hexagonal and the other two pentagonal. The surface is granulous. Primary radials.—Primary radials, three, in each series, about fies as long as wide; each series forming a convex, elevated ridge, con- tracted at the point of the union of the plates; four of the series are supported in the angles, formed at the junction of the basal plates, and the fifth or posterior series is supported upon the middle of the basal plate opposite the azygous side. The plates have about the same length. The third-primary radials are a little wider in the upper part than the others, and support upon the two superior sides the secondary radial series. | | Secondary radials.—The secondary radial or brachial series is con- tinued into the free arms, the first plate has a length about equal to that of a primary radial, the second plate is a little shorter, the third plate about two thirds as long, the fourth plate about half the length, or a little wider than high, the fifth plate about one third the length, and the sixth plate has a length about equal to one half its width. - Above this the plates become shorter, without any noticeable contrac- tion of the width, until the arms are wholly free from the vault, the plates are then cuneiform, and the width is equal to the length of about three plates. . ‘Interradial and inter-secondary radial spaces.—These long, narrow, depressed areas are covered with small plates, having a tubercle or short spine in the central part of each. There are more than seventy- five plates in each interradial area, and twenty-five or more in each in- ter secondary radial area before reaching the top of the cup, but the small plates continue over the margin of the vault, and undoubtedly cover it, and also more or less of the long proboscis, which is extended from the anterior or azygous side. Azygous area.—The azygous area is remarkably large, and covered, in the central part, by a vertical series of plates having about the same size as the regular radial series; and upon each side of the vertical series, there is a ‘depressed area covered by small plates, having a r ‘ | Description of Some New and Remarkable Crinotds. 73 - tubercle, in the central part, as in the regular interradial areas. There are seven plates, each having a length about twice as great as its width, in the vertical series, from the basal plate, upon which the series rests to the top of the vault. This vertical series is continued to the top of the proboscis, and contains in its entire length more than fourteen plates, It has such strong resemblance to the radial series, except as to the branching at the secondary radials, that the general appearance of the body is that of a species having six radial series. Arms and pinnule.—There are ten arms composed of cuneiform plates, the length of three of which is about equal to the diameter of an arm. The pinnule are comparatively coarse, and hence form a dense fringe, upon each side of an arm ; they are long and composed of more than a dozen plates. Some of the lower pinnulz appear to be incorporated into the general body, an appearance noticed in Glypto- - crinus nealli, by Prof. Meek, and in G. richardsoni, by Prof. Wetherby. Column.—The column is quadrangular at the head, but possibly round below. It is perforated at the center by a small, round orifice. The face of each plate contains a central square body, having a diame- ter equal to about half the diameter of the column, which is sur- rounded by a quadrijugous, serrated line, having the angles extended: and the sides depressed or concave, and which in its turn is surround- ed by a smooth, quadrangular margin having concave sides. The genus and species were first studied from two specimens, illus- trated by figs. 3, 8a, and 3b, from the collection of I. H. Harris, Esq., of Waynesville. Ohio, and which were found in the Hudson River Group of that locality. Subsequently I received a specimen for exam- ination, from Dr. D. T. D. Dyche, of Lebanon, Ohio, which shows the azygous side and fourteen plates of the vertical series. From this specimen we learn that the proboscis extends as high as, and probably beyond, the extremity of the arms. And later I received from the collection of Dr. 8.8. Scoville, of Lebanon, the specimen illustrated by figure 3c, which shows very well the character of the pinnule. As the species has been collected at two or three different places, in the upper part of the Hudson River Group, in Warren county, and the quadrangular, columns are not uncommon, at the same range, in Indi- ana, the species may not be so rare as we have been led, hitherto, to suppose. The square column, which I described in the Cincinnati Quarterly Journal of Science, in 1875, and which changes to a round column a few inches below the head, does not, probably, belong to this _ Species. For years collectors have sought for the head belonging to 74 Cincinnati Society of N atural History. the square column, but it was not found until during the past year, and now we have not only two species, but they belong to distinet genera. , GLYPTOCRINUS HARRISI, 0. Sp. Plate I., fig. 4, azygous side, natural sizes fig. 4a, same, magnified two diameters. General form of the body, obconoidal, with slightly depressed inter- radial and axillary areas, as in G. decadactylus. I have not been able to determine with certainty, whether this species has four or five basal _ plates, but as in all other respects it agrees with Glyptocrinus, I sup- | pose it possesses five, each of which is wider than high. If, however, it possesses only four, it would not belong to Xenocrinus, above established, but would still be very closely allied to Glyptocrinus. ‘There are three primary radials in each series. ‘These plates are heptagonal or hexagonal, and of about equal size, as in G. decadactylus. The third primary radial supports upon its upper sloping sides, the , secondary radials of which there are two in each series, as in G. de- cadactylus. From the second of these there arises the two series of brachial plates. the first seven or eight of which are incorporated into and form part of the body. Here the species may be easily dis- tinguished from G. decadactylus, for, in the latter, only one or two plates are incorporated into the body. The increased number of bra- chial plates in the body, at this place, makes it very much longer, proportionally, than G. decadactylus. | There are twenty free arms at the vault, but whether they hifurcate above this or not has not been determined. ‘The interradial series con- sists of one plate in the first range, and two in the second, as in G. decadactylus ; but above this there are many more plates, owing to the increased length of the body, than there are in the latter species. The azygous area is distinguished from that of G. decadactylus, by. _ the increased extension. The axillary areas contain twenty or thirty small plates having a central tubercle on each; and the interbrachial areas have not less than ten or fifteen similar plates in each area. The surface is sculptured, in the lower part of the body, so as to form — triangular depressions between the six star-like radiations from the central part of the plates, as in G. decadactylus; but, above the primary radials, the plates are simply tubercled, and above the second- ary radials not more than a single tubercle occurs on each plate. The column is square, and it is highly probable that the square crinoid column, that I described iu the Cincinnati Quarterly Journal of Science, in 1875, belongs to this species. _ Description of Some New and Remarkable Crinoids. 75 y The species is founded upon a single specimen, from the collection of I. H. Harris, Esq., of Waynesville, Ohio, in whose honor [ have pro- posed the specific name. It was found in the upper part of the Hud- son River Group, at that locality. GLYPTOCRINUS COGNATUS, 0. Sp. Plate I., fig.5, view of the lower part of the body, natural size; fig, 5a, side view, natural size. Body, turbinate; strongly pentagonal in outline, as viewed from be- low; height about equal to the width. There are five sub-basal plates, having a height at the superior angle, in the middle, nearly equal to one half the width of a plate. There are five comparatively large, heptagonal, basal plates, about as wide as high, depressed at the line of junction, and elevated in the central part, thus forming a sub-pen- tagonal outline for this part of the cup. These plates, each, rest upon two of the sub-basals, support upon the upper sloping sides the radials, and upon the superior face an interradial, ; The first primary radial is heptagonal, about as wide as high, and a little larger than either of the others; the second and third are hexag- onal, and a little higher than wide; the three form a convex, elevated ridge, which gives to the body a strong, pentagonal outline, when viewed from below. The third supports upon its upper sloping sides the secondary radials, and upon its superior face an axillary or inter- secondary radial plate. Not less than eight of the secondary radials or brachial series enter into and form part of the body. They gradu- ally diminish in length, so that at about the eighth plate the arms be- come free. Regular interradial areas deeply excavated, and occupied by about _ forty plates, and axillary areas also deeply excavated, and occupied by about twenty plates. The species is established upon a specimen found in the upper part of the Hudson River Group, near Middletown, Ohio, and now in the collection of Dr. R. M. Byrnes, of Cincinnati. The azygous area and character of the arms, unknown. It has a close relationship with Glyptocrinus nealli, though it is dis- _ tinguished by having larger plates, and only about half as many in the interradial and axillary areas. The sub-basals are developed so _ they might be properly called basals, and thus remove the species from _ the genus Glyptocrinus. I have called it cognatus, from its being near _ akin to the nealli, and by some it may be regarded as only a variety, a but comparing it with the specimens in my own collection, I am in- 76 | Cincinnati Society of Natural History. clined to think it is sufficiently distinct to have a specific name. The interradial and axillary plates may have each contained a central tubercle or spine, but our specimen is not in such a state of preserva- tion as to determine this. STROTOCRINUS BLOOMFIELDENSIS. Plate I., fig. 6, natural size, but the underside of the canopy should be dropped down to the dotted lines. (Strotocrinus bloomfieldensis, S. A. Miller, 1879, Jour. Cin. Soc. Nat. Hist., vol. ii., p. 258, pl. XV., figs. 6, 6a.) - This species was originally founded upon a east, but later I re- ceived from W. C. Egan, of Chicago, the matrix, from which a gutta percha cast was taken, and by this means we have the surface mark- ing of the plates completely restored, and are enabled to add to the description. The third radial is octagonal, instead or heptagonal, having a short superior face, upon which an inter-axillary plate is supported. The species most resembles S. regalis, from which it is, however, readily distinguished, by its much shorter first radials, by the octa- gonal third radials, instead of heptagonal, by the presence of the sub- central proboscis, and by numerous minor differences. ‘The ornamenta- tion of the plates, too, is different, though there is great similarity be- tween them, in this respect. It need not be compared with any other known species. ORTHODESMA BYRNESI, 0D. Sp. Plate I., fig. 7, view of the left valve, natural size; fig. 7a, cardinal view, natural size; ye 0s magnified, view of the matrix, showing that the shell was covered by numerous ittle spines. Shell of medium length and breadth, but proportionally very , fie _ Cardinal and basal margins sub-parallel, but gradually diverging pos- teriorly to the posterior third of the shell. The cardinal line is straight, posterior to the beaks, for about one third of the length of the shell, from which point it gradually declines to near the extremity, which is abruptly rounded. Anterior end contracted beneath the beaks, and beautifully rounded in front. Basal line concave in the middle part, for about one half the length. Beaks small, but nearly or quite unit- ing; umbones flattened, and, from which, there is a shallow expanding depression, directed a little posteriorly, and crossing the valves to the basal line. Surface of the valves marked by concentric lines, and covered by ~ numerous little spines. Length, 1 2-10 inches; height, 5-10 inch; thickness, 25-100 inch: The species is founded upon a specimen preserving the shell, and | ae Description of New Fossils from Ohio and Kentucky. Tet also upon the matrix from which the shell was taken, collected by Dr. Rk. M. Byrnes, in whose honor I have given the specific name, in the upper part of the Hudson River Group, near Weisburg, Indiana, and now belonging to his collection. It is peculiar in preserving the mark- ings of the spines-which covered the surface, in the matrix, and also preserving the bases of them on the shell, which may be readily ob- Served with an ordinary magnifier. It will be distinguished from other species by the fact that its thickness is only half its height, and only one fifth its length, as well as by other peculiarities. As this species was covered with numerous spines, it becomes interesting to know whether other species in the same venus were also thus orna- mented. DESCRIPTION OF NEW FOSSILS FROM THE LOWER SILURIAN AND SUBCARBONIFEROUS ROCKS OF OHIO AND KENTUCKY. . By A. G. Wertuersy, A. M., Prof. Geology and Zoology, University of Cincinnati. CEPHALOPODA. Cotpoceras, Hall, 1850, 3d Reg. Rep., N. Y., Birdseye and Black river. CoLPocERAS CLARKEI, nov. sp. (Plate IL., figs. 5, 5a.) Shell very gradually tapering, composed of equal septa, obliquely united at the sides, with a gently rounded convexity pointing to the posterior extremity on the dorsal surface, fig. 5, Pl. II., and an acute angle pointing toward the body chamber on the ventral surface, fig. 5a, Pl. II. The septa are separated by slight semi-sutures, which give the shell a somewhat corrugated appearance, as may be seen in the figures. The obliquity of their line of junction throws the point of the ventral angle of each segment more than three times the width of the segment itself, in front of its posterior dorsal margin. The septa in the speci- men figured have a width of 9 mm. ? In section the specimen is seen to be slightly elliptical, owing to the shortening of the dorso-ventral diameter, which measures 20 mm., while the transverse measures 234 mm. Nine segments of the shell measure two and one half inches, 624 mm., in length, with an almost 78 Cincinnati Society of Natural History. imperceptible difference, 14:mm., in the diameter of the two extremities. Although the specimens are in an elegant state of preservation, so far as the outside marking is concerned, they are silicified, and no evidences of the siphuncle remain. | Remarks.—As this is the second species of this remarkable genus, considerable interest attaches to its discovery. It occurs with the species of Amygdalocystites, Hybocystites, Comarocystites, Apiocy- stites (?), Porocrinus, Hybocrinus, Paleocrinus, Blastoidocrinus, Carabocrinus, Hdrioaster (?), etc., which I have discovered in the Trenton rocks of Mercer county, Kentucky. I have found four specimens, one of which is three times the dimen- - sions of the type herewith figured, and is, no doubt, a different species. I dedicate this rare fossil to my friend, Robert Clarke, Esq., who has assisted me in my labors by the generous donation of his large col- lection of shells, minerals, and fossils, to the University Museum, and also by the use of rare books from his extensive paleontological library, as well as by the warm interest he has always taken in my studies. Cyrrtoceras Goldfuss, 1832. — CYRTOCERAS CONOIDALE, ‘nov. sp. (Plate IL, figs. 6, 6a.) Shell very rapidly tapering, consisting of numerous short septa, of equallength. The specimens which I regard as typical, fig. 6a, Pl. IL, have a comparatively slight curvature. There are seventeen septa in a length of one inch. The siphuncle is small and dorsal. The shell appears to have been exceptionally fragile, as all the specimens which I have seen, except one from the Tennessee locality, are very much distorted by pressure. Remarks.—I1 collected this fossil in August, 1877, at “ Mt. Parnassus,’ Columbia, Maury county, Tennessee; in 1879, at McKin- ney’s station, on the C. 8. R.R., Boyle county, Kentucky; and have since received it from my friend, Mr. W. M. Linney, of Harrodsburg, Kentucky, who collected it in Garrard county. At Columbia it was associated with Stellipora autheloidea, O. lynx, and Crania scabiosa, on the old redoubt excavation of ‘‘ Mt. Parnassus;” at McKinney’s. I collected with it Streptorhynchus filitextus, Ptilodictya hills, Murchisonia bellicincta, and undetermined corals, evidently belong- ing to the Cincinnati Group. At the Garrard county locality, it occurs with P. hilli, and a Rhynchonella, probably a variety of &. capazx. — Description of New Fossils from Ohio and Kentucky. 719 It has been confounded with the C. vallandinghami, S. A. Miller, from which it is entirely distinct. The body chamber being wanting in all the specimens, the diameter can not be determined. I regard the specimen, fig. 6, Pl. IL, as a different species, and nearly allied to C. vallandinghami, S. A. Miller. CYRTOCERAS IRREGULARE, nov. sp. (Plate II., fig. 3). Shell composed of short segments, nearly equal in length and size in the anterior third, gradually becoming shorter and smaller in the pos- terior two thirds. It is moderately curved, the curvature not being well shown in the figure, which is a dorsal view. The specimen is slightly distorted by pressure, but evidences remain that it was some. what elliptical in section from the shortening of the dorso-ventral di- ameter. , The irregularities of form, which are well shown in the figure, char- acterized, likewise, a specimen once shown to me at the University, by the veteran paleontologist, C. B. Dyer, Esq., and which I instantly recognized as being this species. These two specimens are the only ones that have fallen under my observation. ‘The siphuncle is dorsal and comparatively large. The specimen figured, which has a small portion of the body cham- ber, consists of twenty-four septa, and measures 55 mm, in length. The body chamber measures 24 mm. in its greatest, and J1. mm. in its least diameter. The opposite extremity measures 8 mm. and 5mm. in the same diameters, respectively. I collected this species in May, 1877, at Freeport, Warren county, Ohio, in the upper part of the Cincinnati Group. It appears to be rare. Genus Trematopiscus, Meek and Worthen, 1861, Proc. Acad. Nat. Sci., Phil. . TREMATODISCUS KONINCKI, nov. sp. (Plate IL, fig. 4.) ‘Shell consisting of about three coils, formed of about sixty septa, and a partof the body-chamber, measuring 38 mm. in length, on the outer convexity. The septa, as may be seen in the figure, are joined by slightly waved sutures, which have, also, a small dorsal flexure. They are longer on the dorsal than on the ventral side, presenting a somewhat wedge- shaped appearance as shown by the figure. The five septa immediately following the body-chamber are 6 mm. in length on the dorsal surface. 80 Cincinnati Society of Natural History. They are evidently not more than half this on the inner side. They decrease constantly but rapidly in size and length, so that the shell tapers regularly to the apex of the coils. The whole surface is fluted with parallel coarse striz, obliterated in the type, evidently markings of the shell ornamentation, as indicated by other fragments of thesame species. The shell was exceedingly thin and fragile. Its markings are most pronounced on that part of the cast which filled the body- chamber. In transverse section this cavity was nearly circular. Di- ameter of the specimen, measured across from outside of body-chamber, 56 mm., of body-chamber at mouth, as preserved, 20 mm. I collected this fine species, as represented by the type, and several fragments, in the subcarboniferous rocks of the lower Waverly, at King’s Mountain Tunnel, on the C. S. R. R. It was there associated with another, much larger and coarser species, — and with fossils belonging both to the Kinderhook and Keokuk Groups. A fuller study of this part of the subcarboniferous rocks of Kentucky, and more extensive collections of its fossils, which are abundant and well preserved, is very much needed. I hope to make further explora- tions in this region during the coming spring and summer, and hence assign no closer geological limits to the horizon of this fossil for the present. I take great pleasure in dedicating this species to my valued correspondent, Dr, L. de Koninck, of Liege, Belgium, who has done more to develop a scientific and accurate knowledge of the carbonifer- ous fossils of Europe than any other student of its geology. CRUSTACEA, Isocuitina, Jones, 1858, Can. Org. Rem., Dec. 3. IsoCHILINA JONESI, nov. sp. (Plate II, figs. 7, 7a.) GENERAL DESCRIPTION. “Equivalve, the margins of the valves meeting uniformly, not over- lapping as in Leperditia; greatest convexity of the valves, either central or toward the anterior portion. Eye-tubercle present, Mus- cular spot not distinct externally.” Carapace having much the: size and shape of the Leperditia baltica; dorsal margin straight, ventral gently curved. Anterior and posterior margins, rounded. Marginal border very wide at the posterior extremity of the valves, narrowing much anteriorly in the inferior margin, at the center, and widening . again, somewhat, at the anterior side. Valves very convex, with the greatest elevation as seen in profile, sub-central, near to the anterior, * Description of New Fossils from Ohio and Kentucky. 81 dorsal margin. Eye-tubercle very distinct. Muscular spot well indi- cated. Length of medium sized specimen, 22 mm., breadth, 14 mm., ereatest convexity 6 mm., width of margin on posterior border, 34 mm. This beautiful fossil occurs in great numbers, and in high perfection, associated with other species of bivalve crustacea, at a single locality in the Trenton limestone of Mercer county, Kentucky. I have dedi- cated the species to my esteemed correspondent, Prof. T. Rupert Jones, F. R.S., F. G. S., etc., who regards Isochilina as a sub-genus under Leperditia. | ; Proetvs, Steininger, 1830. PROETUS GRANULATUS, nov. sp. (Plate II., figs. 8, 8a, 9, 9a.) Body.—General form elongate elliptical, the cephalic, thoracic and abdominal region being nearly equal in length, the thoracic slightly shorter. Head.—Rounded in front, the angles of the cheeks produced back- ward into short, heavy spines; glabella very prominent, slightly con- stricted near the center, surface granulated, lobed posteriorly; occipital furrow well defined; cheeks margined, the margined space longitudin- ally striated, and much narrowed in front of the glabella; eyes promi- nent, separate from the glabella by a deep groove; entire surface of the head minutely granulate. Thorax.—Consisting of ten (?) segments; axial lobe very prominent, about equal in width to the lateral lobes, the segments slightly arched forward in the middle, nearly or quite equal in length; lateral lobes about as wide as the central, geniculate, with the extremities of the pleura directed backward. Pygidium.—Semi-elliptical, consisting of fifteen (?) segments, axial lobe, prominent, narrower than the lateral lobes,:segments not arched, gradually tapering backward to the margin; Jateral lobes wider in front, tapering posteriorly, widely margined, the margin continuous and granulated. Length of medium-sized specimen, 20 mm.; width across from tip to tip of spines, 10 mm.; length of largest specimen, 26 mm. This may be a different species, but the materials in hand are: not suf- ficient to determine with certainty. This species is not closely enough allied to any hitherto described from American rocks, to make any com- parison necessary. It somewhat resembles P. stokesi, Murchison, of the Niagara Group, but is sufficiently distinct, both specifically and stratigraphically. It is worthy of remark that I have found specimens of this trilobite, 82 Cincinnati Society of Natural History. and of an undetermined Phillipsia, in fossil bodies which I suppose to be the coprolites of the large fishes inhabiting the same seas, and of the magnificently preserved teeth of which I have collected a very large series. I have found, in these bodies, remains of Pentremites, corals, casts of small bivalve molluscs, axes of Archimedes, and small uni- valves. These fishes evidently browsed upon the Bryozoa, and did not dis- dain an occasional crustacean and molluscan morsel. . I collected these trilobites in the Kaskaskia (Chester) Group, sub- carboniferous, Pulaski county, Ky. ECHINODERMA. Genus Hetrrocrinus, Hall, 1847, Pal. N. Y., vol. i. HETEROCRINUS VAUPELI, nov. sp. (Plate IL., figs. 1, 1a.) Of this remarkable species we have but asingle imperfect specimen, consisting of the middle third of the rays. No part of the body, column, or upper part of the arms has been seen. The plan of the species is very much like that of H. constrictus, Hall. The arms are comparatively heavy, ten in number, and com- posed of plates which are slightly longer than wide, but so nearly equal in these two dimensions 4s to give them a very. regularly quad- rate form. At the sutures joining the plates, as may be seen in fig. la, Pl. IL, there are ridges running across the arms, which join lateral ones belonging to the arms themselves. As these elevations are raised above the general surface of the arms, about one third the thickness of the latter, the effect is to give the crinoid a beautifully reticulated ap- pearance, well shown inthe figure. In several very perfect specimens of the H. constrictus, which I have studied, the ‘‘ armlets’”’ (Meek, Ohio Pal., vol. i., p. 3), subdivided on the second, third or fourth piece, the place of the division being somewhat irregular in the upper part of the arms. In this species there are no subdivision of the armlets, which are much more delicate than those of the H. constrictus. ‘The method of origin of the armlets is nearly alike in the two species, so far as can be determined by the specimen. In H. vaupeli the armlets are long and gradually tapering to the extremity. There are no evidences of ordinary pinnule. As this is also the case in the H. constrictus, so far as Ihave been able to determine from very perfect specimens, I am of the opinion that these two species should be set aside as very distinct from Heterocrinus proper. The Description of New Fossils from Ohio and Kentucky. 83 origin of the armlets, the absence of true pinnule, and the presence of a long proboscis, are characters very different from those belonging to the H. simplex, which may be regarded as the type of the genus. I dedicate this beautiful and unique fossil to its discoverer, Mr. Ernst H. Vaupel, of this city, who has collected many of our rarest fossils, and who is devoting especial attention to our corals. Genus Rereocrinous, Billings, 1858, Can. Org. Rem., Dec. 4, Under this generic name, Mr. Billings described two species from the Trenton rocks of Canada, in the publication cited above. Like most of the fossils of the locality whence they were obtained, these were in a very poor state of preservation. Enough is shown, however, by Mr. Billings’ figures, to make it conclusive that several forms of our so called Glyptocrinus should be referred to this genus. Among them I should place G. nealli, Hall, G. richardsoni, Wetherby, and the species of which the description is to follow. Not wishing, however, to be too hasty, I now include, under Reteocrinus, only L. richardsoni and &. gracilis. I may add, in order to give authority to this deter- mination, that the same opinion is held by Mr. Wachsmuth, of Bur- lington, Iowa, who will so group these species in his forthcoming vol- ume on the Paleocrinoidea. RETEOCRINUS GRACILIS, nov. sp. (Plate IL, fig. 2a, azygous; 2, op- posite side). Underbasals.—-Five, very small, nearly concealed between the column and the greatly developed basals. In the size of these plates this species agrees with R. nealli. Basals—Five, hexagonal, somewhat higher than wide, squarely truncated above, and here forming the base of the interradial space. The outer angles of the upper extremity are cut off, forming the articu- lar surface for the support of the first radials. From the ‘lateral angles thus formed near the center of these plates, they narrow gradu- ally to the lower extremity which is rounded. The widest part of the plates is at this lateral angle, so that the basals do not join at the sides below this point, leaving a suture through which the minute underbasals and the top of the column may be seen, and over which the center of the first radials rests. The basals are thick and heavy plates, the one on the azygous side being slightly wider and shorter than either of the other four, Radials—First series, five, pentagonal, higher thau wide, squarely 84 Cincinnati Society of Natural History. truncated above, the sloping inferior sides resting between the basals. The lowest point of these plates, which is on a line with the suture joining the basals, is slightly excavated, giving the lower end a bifur- cate appearance. The interradial sides are depressed, leaving an ele- vated central ridge to this part of the ray which is thus continued throughout the radial and brachial series. Second radials—Five, quadrangular, higher than wide, equal in size, squarely truncated above and below, lateral margins depressed. Third radiais—Five, pentagonal, higher than wide, wider above, with two articulating surfaces upon which the rays divide. Lateral edges depressed into the borders of the interradial spaces, upper mar- gin slightly excavated between the articulating faces, giving the plate a bifurcate appearance. Brachials—First series, ten, quadrangular, higher than wide, equal in size, and alike in form. Second series, ten, pentagonal, higher than wide, wider above, with two articular facets, upon each of which an arm originates, a slight excavation occupying the space between these facets. Arms—Twenty, long, slender, composed of equal, quadrangular plates, about as high as wide, without bifurcation or divisions. . Pinnule—Long, delicate, and originating on alternate arm plates either side of the ambulacral groove. Vault—Unknown. Anal and interradial spaces filled by an indefinite number of small, delicate, generally hexagonal plates. Among these may be detected those of the “fixed pinnule,” to which I called attention in my de- scription of Reteocrinus richardsoni. I have great pleasure in again acknowledging the bigh character of the work done by Mr. Billings, whose keen discrimination detected the generic value of the imperfectly preserved specimens with which he had to deal. This beautiful fossil was discovered in Lime Kiln Hol- low, formerly a noted collecting ground, by Ernst H. Vaupel and Mr. John Nickles, to whose kindness I owe this opportunity of de- scribing it. Nore oN THE TRENTON Fossits oF MERCER Co., Ky. Since publishing my article on the Trenton Limestone of Kentucky (this JournaL, July, 1880), I have discovered many rare additional forms. Among them must be noted a large species of Comarocystites; Life and Character of George Graham. 85 several species of Crinoids, as yet unstudied; a fine specimen of A teleo- eystites (?) and several very fine trilobites. When it is remembered that two years since nothing was known of the fossil contents of these massive Kentucky river limestones, it is gratifying to be able to re- cord such progress, in working out the evidences of their age as deter- mined by their fossils. Much, however, remains to be done in refer- ence to the lower part of the section, which proves to be full of fossils, though the localities containing well preserved specimens are very few. It is quite certain, however, that the lowest part of the section at High Bridge is either very low [Trenton or even Chazy. During the present season I hope to accomplish such discoveries of fossils as will determine this question satisfactorily. The new life which tke Kentucky Geological Survey has, under its present com- petent Chief Geologist, Hon. John R. Procter, will, I am sure, add much to the facilitating of this work. REPORT OF THE COMMITTEE ON THE LIFE AND CHARACTER OF GEOKGEH GRAHAM. The committee appointed at the last regular meeting of the Cincin- nati Society of Natural History, to prepare a notice of the life of Mr. George Graham, a prominent citizen of Cincinnati, and a life member of this Society—begs leave respectfully to report: That Geo. Graham, who died March Ist, 1881, in the 83d year of his age, was born at Stoyestown, Somerset county, Pennsylvania, in November, 1798; that he was the son of George and Elizabeth Gra- ham; and that his father was an officer in the Pennsylvania Volun- teers, in the War of 1812. The son accompanied his father when he marched a regiment to the defense of Black Rock in Canada, acting as clerk and making out payrolls. On his return from this expedition he went into the dry goods business with his brother; but in 1816 we find they had contracted to build the first turnpike road over the Alleghany mountains, and agreed to haul merchandise from Philadel- phia to Pittsburg in ten days. Thus, at the early age of 18 years, we find him engaged in those public enterprises which introduced a life of usefulness, as his subsequent career will show. In 1822, he came to Cincinnati, at that time a comparatively small frontier settlement; and from that time until his death he was an active and useful citizen. On his arrival here he entered into partnership 86 Cincinnati Society of Natural History. with M. P. Cassilly, and George M. Davis, and engaged in the hard- ware business. This partnership lasted but three months, when, in consequence of some disagreement, Mr. Graham retired from the firm. His next venture was to supply troops at Prairie du Chien and Fort Snelling with army supplies. In 1823, he returned to Cincinnati, and formed a partnership with C. W. Gazzam, and engaged in the commis- sion and steamboat business, the firm acting also as agents and build- ers of boats in the Cincinnati and New Orleans trade. He was a leading Mason, and was one of the charter members for the organization of the LaFayette Lodge, to receive the distinguished foreigner, Marquis de LaFayette; and when, in 1825, the illustrious Frenchman came to Cincinnati, Mr. Graham delivered the welcoming , address; and in 1827 he took the 33d degree of the Scottish Rite, and was one of seven who organized the Scottish Rite Consistory in Ohio, now numbering 700 members. In May, 1817, Mr. Samuel W. Davis obtained from the Legislature of Ohio, a charter to supply the city of Cincinnati with water for 100 years, He was, however, unable to keep to his contract, and in 1825 . offered to sell to the city his charter, and ten acres of ground with im- provements for $20,000. The offer was rejected. Mr. Graham witha - far sightedness, remarkable in a young man of 27, saw the importance of the project to the city, and with John P. Foote, Wm. Green, Davis’ B. Lawler, and Wm. 8. Johnston, purchased what the city had refused, for $30,000. Five times during the next fourteen years, the city de- sired a price to be set upon the works, and in 1839 purchased them for $300,000, just ten times the original cost. In 1827, Mr. Graham was married to Miss Ellen F. Murdoch, of Urbana, Ohio. He had five children by the marriage, only two of whom are now living, Mr. Robt. M. Graham, and Lavinia M., the wife of Mr. John M. Newton, Librarian of the Young Men’s Mercantile Library Association. In 1829, he was elected to the Legislature, and while there, as chair- man of the Finance Committee; detected and rectified abuses and frauds which had existed for some years. In 1829, he, in connection with A. Richards, was the owner of the first cotton mill in Dayton, Ohio, and of the first carpet factory west of the Alleghany mountains. At the same time he carried on a foundry for making cotton mills and other machinery. In 1835 he made a contract with some Mexican capitalists, to build and put into operation machinery for making fine cambric muslins in the Durango P Life and Character of George Graham. 87 District in Mexico, 900 miles from the sea coast. This machinery had to be made in pieces of about 100 pounds, in order to be transported over the mountains on the backs of mules. In 1832, Mr. Graham was elected trustee of the public schools; and as such made many needed reforms, and introduced new regulations. He constructed rules for the government of schools, teachers, and scholars. These were printed, framed, and hung up in every school house. He introduced the system of school examinations, and used to march at the head of the procession of children through the streets on the last day of school, to some church where rewards of merit were distributed by the mayor. In 1834, he applied to the city government for funds to build a model brick school house for 500 pupils. The council had proposed to erect a wooden house of two stories for $1,200. This did not suit Mr. Graham, who said he did not wish to see the scholars burned to death in a trame building. Following his own ideas, he appointed an architect to erect a brick school house, and guaranteed payment in case the city refused. The building was completed in 1854, afterward re- modeled and enlarged, and still stands on Race street, opposite the. Arcade, devoted to other than educational purposes. Eight other school houses were soon erected in various wards of the city, by money procured on bonds, payable 25 years from date. About the same time, | he, with John P. Foote and Calvin Fletcher, organized the Mechanics’ Institute. For several years the three paid the rent of a building suitable for the purpose. In 1836, Mr. Graham and other citizens fitted out a body of troops, and sent them to Texas to defend it from the threatened invasion of Santa Anna. These troops, with a regiment from Louisville, comprised the main part of the army which fought at San Jacinto under Generals Sherman and Houston; the army captured Santa Anna, thus securing the independence of Texas. In 1838, he was elected President of the Jeffersonville Association, which was organized in 1836, to build-a canal around the Falls on the Indiana side of the Ohio. Five hundred and forty acres of land were laid off in lots. Surveys were made by the company and by Col. Long, U.S. engineer; and from these surveys it was estimated that for $1,800,000 a canal 60 to 80 feet wide, with locks 400 feet in length, to pass the largest boats, could be built. This was about the amount re- quired to enlarge the Louisville canal. During two sessions of Con- eress, Mr. Graham was in Washington, and labored hard to get aid for 88 Cincinnati Society of Natural History. the passage of a bill for the company. Southern influence was too strong for him, and the bill failed. He was mainly instrumental in building the Cincinnati and Miami- town, now the Cincinnati and Harrison pike, and macadam- ized it by means of steam machinery. He also, we believe, was the first to point out that it was possible, by means of gravel alone, to make nearly as good a road as could be made with broken stone. The Western Academy of Natural Sciences was founded in 1835. Mr, Graham was present at the first called meeting, held at the hall of the Medical society, April 25th of that year. He was one of the committee appointed to prepare a constitution and by-laws, and he was one of those named in the act of incorporation of the academy, Feb. 22, 1836. Afterwards he was, for a number of years, President, in which position he took an active part in all its affairs.* After the formal suspension of the meetings of the academy, and the deposit of its effects in the present Cincinnati Society of Natural History, Mr. Graham was, with several other members of the old organization, elected a life member of the present association. He found time, dur- ing the many occupations of a busy life, to make collections of shells, fossils, and plants. ‘These were subsequently destroyed by a fire in a warehouse where they were stored. Up to the time of his death he was constantly on the alert for objects of interest to add to his cabinet. Cincinnati is acknowledged to be the first city in the United States where steam fire engines were used. When it was announced that the city had such engines, all the other large places in the country ridiculed the idea. It was insisted that nothing better than the old fashioned fire engines could be had. Atthat time this city possessed a volunteer Fire Department of 3,000 members: and they were governed by laws of their own, and had everything much as they desired. Mr. Graham’s early connection with the Water Works, and his active participation in the Fire Department, as chairman of the committee on Finance in the City Council, caused him to suggest the employment of steam fire en- * Mr. Graham was the last survivor, but one (Wm. D. Gallagher being now the only one living), who participated in forming the Academy. Believing it may be of interest to many we append a list of names of those taking part in the organization of the Western Academy of Natural Sciences at Cincinnati, at the first meeting, in the order, and as we find them recorded: R. Buchanan, Dr. Whitman, J. Hall, W.D. Gallagher, Dr. Shotwell, Dr. Colby, Dr. Drake, G. Graham, Dr. Wood, Dr. McDowall, Dr. Gross, Dr. Marshall, Dr. Riddell, J. H. Perkins, Mr. Clark, Dr. Mason, Mr. Hells, J.S. Armstrong, P. Symmes, Dr. Locke, —— Flagg. R. Buchanan acted as Chairman, andJ. H. Perkins, as Secretary. oe Life and Character of George Graham. . 89 _ gines. He engaged A. B. and E, Latta to make a machine for an ex- periment, not to cost more than $400. If successful the city was to purchase the engine. Ata public trial, Mr. Miles Greenwood, Mr. Geo. Graham, and Mr. Jos. Ross, officiated as masters of ceremonies. The experiment was a complete success, and the “ Bull of the Woods,”’ as it was called, raised steam in five minutes, and threw water a dis- 2 tance of fifty feet from an inch nozzle, . At the very next meeting of the council, $5,000 were voted for the purchase of steam fire engines. From the “ Bull of the Woods” as a foundation, sprang the present efficient and invaluable system for extinguishing fires. Mr. Graham was one of the incorporators of the Cincinnati Horti- cultural society in 1845. Previous to that, he had, in 1844, contri- » buted a paper on “ Fire Blight,” which appeared in the Proceedings _, of the Society. He held various offices at different times; was Presi- . dent in 1847, and was re-elected in 1870. He always took an active interest in its proceedings. He was for several years trustee of Woodward and Hughes High Schools, and one of the early trustees of the Cincinnati College, holding that position for forty years. In 1863, when the Great Western Sanitary Fair was held in this city, Mr. Graham was very active. He was the Chairman of several Committees, and was the chief author and compiler of the 578 page report of the Fair. He personally ‘attended to the unpacking, arrang- ing and labeling of some 1,200 articles exhibited in one of the depart- ments; and much credit is due him for his untiring energy. In 1867, he visited Europe, spending sometime there, and meeting with various adventures. In 1869, he was one of a congratulatory party which went from Cincinnati to San Francisco when the Pacific railroad was completed. He visited various parts of California, and ~- spent some time in Yosemite valley. A paper written by him, de- scribing the trip, shows Mr. Graham to have been a man of large in- formation, as well as an acute observer. U. P. JAMES, A. J.. HOWE, Committee. O. D. NORTON, M.D., 3 The funeral of Mr. Graham took place from the Church of the New _ Jerusalem, on the corner of Fourth and John streets, on the 4th of March. The casket was borne to the hearse by John D. Caldwell, L. aad, ae 3 my Ete © . ps 4 Ay a 3 t ~~ ¥ » * % ’ ee x ‘4 < - ? 90 Cincinnati Society of Natural History. | J. Cist, Julius Dexter, John Carlisle, Henry Urner, and A‘ T. Gos- horn. He was interred in the Graham lot in Spring Grove. | He has been described as a man of remarkable appearance, having clearly-cut classical features, positive Roman nose, finely-cut mouth, and decisive chin, with the old-time gentleness of manner which would have attracted attention in any country. Here, when strangers or. younger persons inquired as to who the remarkable-looking old gentle- man might be, they simply learned that it was George Graham, an old citizen. He was identified with or interested in all the recent events that have tended to improve the metropolitan character of the city, and especially in the musical and esthetical culture. . He attended his jast Operatic Festival only the Saturday evening before his decease, when, it is supposed, that some slight exposure caused him to contract. the indisposition which proved fatal in three days. | He was for many years an active member of the Chamber of Com- merce, of this city, and later in life, in compliment of his eminent services in public affairs, in earlier periods, he was elected an honorary life member of that influential body of merchants. The Chamber, in its ‘memorial giving the expression of their members upon his life and character, says : | “Mr. Graham was always a close observer and thinker, a devoted student of nature, and a careful reader of books. He thus acquired a great fund of knowledge, both scientific and practical. He was a man of great general information, and possessed a happy faculty of imparting knowledge to others in a manner fascinating to friends, Even after all active participation of his with enterprises, the efforts of younger men to advance the interests of and build up the city of his adoption, met with his hearty sympathy, as though these efforts were the reflex in his later life of the courage and integrity with which his ca- reer was marked in earlier days.” PPO ee hy Tak ew 4 ha ee a, dy q THE JOURNAL PNGTANATISCIEY OP NATURAL HISTIRY PROCHEDINGS OF THE SOCIETY. Turspay Evenine, April 5, 1881. Dr. R. M. Byrnes, President, in the chair; L. 8. Cotton, Secretary pro tem. Present, 28 members. James R. Challen and R. A. Holden were elected members of the Society. | This being the annual meeting, the Treasurer made his report, show- ing the funds of the Society, and the income and disbursements of the past year. Other officers of the Society made verbal reports. The Society elected for the ensuing year the following officers: President—R. M. Byrnes, M.D. First Vice-President—J. H. Hunt, M.D. Second Vice-President-—Prof. Ormond Stone. Secretary—F. W. Langdon, M.D. Treasurer—S. E. Wright. Librarian—S. A. Miller. Curator of Mineralogy—J. W. Hall, Jr. Paleontology—J. Mickleborough. Conchology—E. M. Cooper. Entomology—Harry J. Hunt. Botany—O. D. Norton, M.D. Ornithology—J. W. Shorten. Ichthyology—D. $. Young, M.D. Archeology—H. H. Hill, M.D. Comparative Anatomy—A. J. Howe, M.D. Herpetology—A. E. Heighway, Jr. 92 Cincinnati Society of Natural History. Members at large for the Executive Board, Prof. G. W. Harper, C. F. Low, H. H. Hill and J. Mickleborough. Trustee—R. B. Moore. A committee consisting of R. B. Moore, U. P. James and Dr. O. D. Norton, was appointed to report suitable expressions of the Society on the death of Mr. David Bowles, a life member. Turspay Evenine, May 3, 1881. Prof. Ormond Stone, Vice-President in the chair; F. W. Langdon. Secretary. Present, 12 members. | H. M. Schultz was elected a member of the Society. The committee on the Death of Mr. David Bowles was reauested to prepare its report in time for publication in the July No. of the JOURNAL. The Smithsonian Institution presented six volumes of Contributions to Knowledge—vols. 16 to 21 inclusive. Captain L. Barney, vol. 1 of the Proceedings of the Natural History Society of Paris, 1792. E. A. Pohlmeyer an Anaconda, in alcohol. And Joseph F. James some Lepidopterous insects. Turspay Evenine, June 7, 1881. Dr. R. M. Byrnes, President, in the chair; F. W. Langdon, Secretary. Present, 20 members. Remarks were made by Dr. D. 8. Young upon the fossil fish pre- sented by Mr. Charles DeYoung, of California, through the kindness of Mr. Murat Halstead, of the Cincinnati Commercial, Col. P. P. Lane, of Norwood, in Hamilton county, presented to the So- ciety his collection ofrelics from the ancient cemetery at Madisonville, which embraces several hundred specimens; Dr. C. L. Metz also pre- sented a collection from the same locality; Davis L. James, 33 species of seeds of Cincinnati plants; Dr. A. J. Howe, a Septaria and a Medi- cal Journal; Jos. F. James, 1 box of insects, catalogue of fossils in Heidelberg Mineralogical Institute, and 4 magazines; Mr. E. P. Cranch, an old Cincinnati collector of specimens of Natural History, 22 boxes of fossils, largely from the hills at Cincinnati, 9 boxes of minerals, 6 boxes of shells, some of them quite rare, and 2 boxes of mosses and lichens, and a lot of Pine cones, etc., etc.; Mr. Geo. Skinner, of Kalida, Ohio, a photograph of Indian relics; U. P. James, Paleontologist No. 5; E. H. Vaupel, 42 species of Cincinnati fossils; S$. T. Carley, of Bantam, Clermont Co., O., a slab of Glyptocrinus decadactylus, and labrum of an Asaphus; Charles DeYoung, of San Francisco, California, through Murat Halstead, Esq., a beautiful fossil fish; from Wm. Hubbel Fisher, 2 skins of Hylotomus pileatus; and from Dr. O. D. Norton, Michaux’s N. Am. Sylva, 3 vols., Browne’s Sylva Americana, and Barton’s Ele- ments of Botany, 3 vols. Mesozoic and Cenozoic Geology and Paleontology. 5) THE CANOZOIC AGH OR THERTIARY PERIOD. By S. A. Mirrer, Esq. [Continued from Vol. iv., page 46.| Before reaching Bridger station the strata on either side of the road are horizontal, or nearly so. A long, flat ridge extends down a little east of north from the Uinta mountains, between Black’s Fork and the Muddy. ‘This may be regarded as the geological divide be- tween the waters of the Great Salt Lake Basin and the drainage of Green river. The Muddy is one of the branches of Black’s Fork, which flows into Green river, and west of this stream we have what is called the eastern rim of the Great Basin of Salt Lake. If we were to travel southward to the foot of the Uinta mountains, from the rail- road along this divide, we should be able to detect no well-marked line of separation between the Green River Group and the Wasatch Group. Bridger’s Butte, as well as the entire eastern portion of this divide fronting the valley of Black’s Fork, exhibits a large thickness of the somber, indurated sands, clays, and sandstones of the Bridger Group, passing down into light buff, chalky layers, with Planorbis, Unio, He- lix, Goniobasis, etc. Within a distance of ten miles to the west of this butte the little streams cut through the pinkish beds of the Wasatch Group, then pass up into whiter, indurated, marly clays, with numer- ous concretionary layers, differing from the chalky beds of the Bridger and Green river basin. This divide probably forms the junction of two great fresh-water lake basins, that may have existed contemporane- ously. The two great basins may have been connected with each other at different points at some stages of their growth, but there is an abrupt, persistent, very marked difference in the character of the sediments of the two basins. While the Green River and Bridger Groups abound with fossils, the Wasatch Group, like all the rocks of the west that are characterized by brick-red coloring matter, is compara- tively quite barren. At Bridger station, and from Bridger to Aspen, which is about 24 miles, the ochreous beds of the Wasatch Group are - well exposed on both sides of the road, and the valley through which the road passes from Piedmont to Aspen is carved out of this Group The tunnel at the head of Echo canon is cut through the reddish and purplish indurated sands and clays of the Wasatch Group. It is 770 feet in length. The valley of Echo canon is one of erosion, and on either side the rocks rise wall-like 500 to 1,000 feet, or have been weathered into curiously castellated forms, and bear such names as os) Cincinnati Society of Natural History. Witches’ Rock, Eagle Rock, Hanging Rock, Conglomerate Peak, Sen- tinel Rock, Monument Rock, etc. Monument Rock is a regular obelisk of conglomerate, standing at the junction of the Echo with the Weber valley, and being about 250 feet high. Descending the Echo canon, the more rugged picturesque scenery is exhibited on the right hand, and descending the Weber the same lofty perpendicular walls; weathered here and there into all sorts of fantastic forms, continue to the Narrows, where the Weber river makes a bend to the left, and the conglomerates disappear. The whole series of these beds is referred to the Wasatch Group, and the thickness estimated at from 3,000 to 5,000 feet, the conglomerate portion being from 1,500 to 2,000 feet. He proposed the name of the “ Sweetwater Group,” for a lake deposit found in the Sweetwater valley. There is a high ridge or divide, between the drainage of Wind river, North Platte, and Sweetwater, 300 to 400 feet above the channels of these streams, which is com- posed ofthe Tertiary beds. The Sweetwater forms a distinct concavity, with this high divide on the north and east, and the valley has been scooped out so that until we reach the Sweetwater Canon, near the South Pass, only the massive granite ridges rise up among the modern Tertiary beds, which jut close up against their base. This is a valley of denudation, over a space of at least 30 to 50 miles in width. All the unchanged formations, from the lignite Tertiary down to the massive feldspathic granites, have been worn away, leaving the granites scat- tered over the valley in the isolated ridges. At that time there was a fresh-water lake which occupied the entire valley, much as Salt Lake once occupied the.great basin, concealing most of the granite ridges, while others rose above the waters like islands. Then was de- posited what he called the Sweetwater Group, or perhaps a series of beds identical with the upper portion of the Wind river deposits. These were scooped out again in time, and the Pliocene marls and sands were deposited; and then again there was another scooping out of the valley, and finally a covering of the hills with drift. The mountainous portions of Northern Utah* are full of beautiful park-like areas, which contain the evidences of an ancient lake. At Copenhagen there is a considerable drift or bowlder deposit with fine white or yellow marly sands and clays, in regular layers, showing the deposit to be Post-pliocene, and that the waters of the lake were com- paratively quiet. Near Box Elder Canon are two kinds of terraces, * U.S. Geo. Sur. of Montana, ete. ‘Mesozoic and Cenozoic Geology and Paleontology. 95 - the usual lake terraces, of which there are two well-defined lines at least, and the river terraces, which are confined to the streams, and do not seem to have any direct connection with the former. The lowest plain valley opposite the canon, near the water’s edge, is 4,344 feet above sea level; 1st terrace, 4,683 feet; 2d terrace, 4,776 feet; and 3d terrace, 3,858 feet. These terraces show the gradual decrease, step by step, of the waters of the ancient lake, and the operations of the little streams pouring into it from the mountains on either side. The amount of local drift that has been swept down through the gorges or canons and lodged at the opening is very great. At the immediate mouth of the canon, the bowlders are quite large, varying in diameter from a few inches to several feet. Westward toward the shore of the lake the bowlders diminish in size and quantity, and the finer sedi- ments, as sands and marls, increase, showing a constant decrease in the power of the currents of the water after leaving the mouth of the canon. The local drift is conspicuous in Logan Canon. It is composed of rounded bowlders, with clays and marls, reaching a thickness of 100 to 150 feet in regular and horizontal strata, attached to the sides of the gorge, and showing that, however turbulent the waters, the materials were deposited in a lake, At the entrance of the canon are some re- markable terraces, composed of sands, clays, marls and rounded bowlders. A large portion of Utah is made up of nearly parallel ranges of mountains, trending nearly north and south, with intervening valleys of greater or less width, which, after their elevation, formed shore lines for detached lakes or bays. It would appear that the last lake-period of this portion of the west commenced in the Pliocene epoch, and con- tinued on up to the present time; that the waters once filled all these valleys, so that they rested high upon the sides of the mountains, de- positing what Prof. Hayden called the Salt Lake Group, gradually passing into the Post-pliocene deposits which verge upon our present period. It is quite possible that there have been oscillations of leve] in these modern lake-waters; but so far as the proofs go, this great in- land lake may have continued quite uniform until the terrace epoch, and that then the waters gradually receded to their present position. The immediate valley of Bear river, near the crossing, is interesting on account of the fine development of the lake-deposit, which is com- posed of clay, sand, and marl, yellow and rusty-drab color, and attains . a thickness of 200 to 300 feet. The elevation of Bear river valley, at 96 Cincinnati Society of Natural History. the bridge, is 4,542 feet, and the highest terrace on the east side is 4,737 feet, and the highest on the west side is 4,779 feet. The imme- diate valley of Bear river may be said to have been worn out ofthe Plio- cene or lake deposit. Among the lower ranges of hills that border the east side of the Great Snake river basin, especially from Port Neuf Canon northward, the Pliocene deposits are well shown, and lie beneath the basaltic floor. In the Port Neuf Canon this fact is illustrated by the wearing away of the cap or floor of basalt, in a number of localities, but on the sides of the hills this is shown with equal clearness by the elevations of the basalt. The dip of the beds is not great, usually not more than 5° or 10,° and in all cases in the direction of the great basin. This would indicate that there had been a moderate elevation of the mountain ranges, or a depression of the basin at a very modern date, even ap- proaching very close to our present period. The effusion of such a vast amount of igneous matter from the interior of the earth, might suggest the possibility, or even probability, that the cause of the subsequent changes in the hills around the borders, was either contemporaneous or subsequent to the effusion of the melted material. If the elevation began with the eruption, it certainly continued long after it ceased, in- asmuch as the basalt is lifted up in thick beds, at the same angle with the underlying strata. Not only in the valley of the Port Neuf and Snake river is the basalt found in conjunction with lake deposits, but in numerous localities all over the northwest, it seems to rest upon these Pliocene beds, readily adapting itself by the form of the under surface to the irregularities of the surface of the lake deposits. Prof. Eug. W. Hilgard* divided the Eocene of Alabama and Missis- Sippi in descending order, into, lst, Vicksburg Group, 120 feet; 2d, Red Bluff Group, 12 feet; 3d, Jackson Group, 80 feet; 4th, Claiborne Group, 60 feet; 5th, Buhrstone Group, 150 feet; 6th, Flatwoods and Lagrange Lignitic Group, 450 feet, making a total thickness of 872 feet. The Lagrange and Porter’s Creek Group of Safford is the same as the Flatwoods and Lagrange Lignitic. The Buhrstone Group of Tuomey is the same as the Siliceous Claiborne Group of Hilgard. The Kocence is followed by the Grand Gulf Group, probably a de- posit in brackish water, almost non-fossiliferous, and having a thickness of 250 feet. Prof. Leo Lesquereuxt described, from the Green River Group of * Proc. Am. Ass., Ad. Sci. + 1872, U. S. Geo. Sur. of Montana, ete. ae) — Mesozoic and Cenozoic Geology and Paleontology. ot Wyoming, high on hills from the river, Ceanothus cinnamomoides, now Zizyphus cinnamomordes ; from the Bridger Group at Washakie station, near Bridger’s Pass, Rhamnus intermedius, Liquidambar gracile, now Aralia gracilis, and Quercus emulans; and from Barrell’s Springs, Hquisetwm hayden. After reviewing the state of the knowledge of the Tertiary and Cre- taceous flora of this country, he arrived at the following conclusions, to-wit: 1. The Tertiary flora of North America is, by its types, intimately related to the Cretaceous flora of the same country. 2. All the essential types of our present arborescent flora are al- ready marked in the Cretaceous of our continent, and become more distinct and more numerous in the Tertiary; therefore the origin of our actual flora is, like its facées, truly: North American. 3. Some types of the North American Tertiary and Cretaceous flora, appear already inthe same formations of Greenland, Spitzbergen, and Iceland; the derivation of these types is, therefore, apparently, -from the arctic regions. 4, The relation of the North American Tertiary flora with that of the same formation of Europe, is marked only for North American types, but does not exist at all for those which are not represented in the living flora of this continent. Therefore, the European Tertiary flora partly originates from North American types, either directly from our continent, or derived from the arctic regions. 5. The relation of the Tertiary flora of Greenland and Spitzber- -gen with ours indicates, at the Tertiary and Cretaceous epochs, land connection of the northern islands with our continent. 6. The species of plants common to the Cretaceous and Tertiary formations of the arctic regions, and of our continent, indicate, in the mean temperature, influencing geographical distribution of vegetation, a difference, in +-, equal to about 5° of latitude for the Tertiary and Cretaceous epochs. 7. The same kind of observation on the geographical distribution of vegetable species, shows at the Tertiary and Cretaceous times, differ- ences of temperature according to latitude, analagous to what is re- marked at our time, by the characters of the southern and northern vegetation. Prof E. D. Cope* referred the Bridger Group to the Eocene, and de- scribed, from Cottonwood creek, Wyoming, Mesonyx obtusidens, Triaco- - * Pal. Bull., No. 1, and Proc. Am. Phil. Soce., vol. xii. 98 Cincinnati Society of Natural History. don aculeatus, Lophiotherium pygmeum, Anostira edemia, now Plas- tomenus edemius, A. molopina, now P. molopinus, A. trionychoides, now P. trionychoides, Trionyx concentricus, T. thomasi, now Plasto- menus thomast, Axestus byssinus, Bena hebraica, Testudo hadriana, now fladrianus corsoni, Emys polycyphus, EH. terrestris, Helothe- rium procyoninum,* Stypolophus pungens, Pantolestes longicaudus, Pseudotomus hians, Hadrianus octonarius, Hadrianus allabiatus,t Protagras lacustris; from the Bad Lands of Black’s Fork of Green river, Wyoming, Stypolophus brevicalcaratus, S. insectivorus, Miacis parvivorus, Tomitherium rostratum, and Emys latilabiatus. He described,} from the Eocene of the upper waters of Bitter creek, Wyoming, Synoplotherium lanius, Crocodilus clavis, Rhineastes pelta- tus, R. smithi, Loxolophodon cornutus,§ L. furcatus, L, pressicornis, and Palewosyops vallidens. From the northern part of the Eocene basin of Green river, Anaptomorphus emulus,|| Crocodilus sublatus,4 C. sulciferus, and Anostira radulina. From the lower beds of, the Green River Group, near Black Buttes, Alligator heterodon. From the Wasatch Group, near Evanston, Utah, Bathmodon radians,B. semt- cinctus, Notharctus (now Hyracotherium) vasacciensis, Notomorpha gravis, N. testudinea. From the Eocene, at Osino, 25 miles northeast of Elko, Nevada, Trichophanes hians and Amyzon mentale. From the Green River Group of Wyoming,** Hrismatopterus rickseckert, and Os- teoglossum, now Dapedoglossus encaustum. He described, from the Eocene of New Jersey,}+ Lembonax propyleus, L. insularis, and Thecachampsa serrata. And from the Miocene near San Diego, California, Hschrichtius davidsoni. Prof. O. C. Marsh described,{t from the Eocene near Fort Bridger, and near Henry’s Fork, Wyoming, Palwosyops laticeps, Telmathert- um validus, Hyrachyus princeps, Homacodon vagans, Lim- nocyon verus, Viverravus gracilis, Nyctitherium velox, N. priscus, Talpavus nitidus, Limnofelis ferox, IL. latidens, Limnocyon riparius, L. agilis, Thinocyon velox, Viverravus (?) nitidus, Thino- lestes anceps, Telmalestes crassus, Limnotherium affine, Orohippus * Pal. Bull. No. 2, and Proc. Am. Phil. Soe. + Pal. Bull. No. 8, and Proc. Am. Phil. Soe. t Pal. Ball. No. 6, and Proc, Am. Phil. Soe. 2 Pal. Bull. No. 7, and Proc. Am. Phil. Soe. || Pal. Bull. No. 8, and Proc. Am. Phil. Soc. q Pal. Bull. No. 9, and Proc. Am. Phil. Soc., vol. xii. * U.S. Geo. Sur. of Wyoming. ++ Proc. Acad. Nat. Sci., Phil. tt Am. Jour. Sci. and Arts, 3d ser., vol. iv. ses Mesozoic and Cenozoic Geology and Paleontology. 99 “pumilus, Helohyus plicodon, Thinotherium validum, Passalacodon litoralis, Anisacodon elegans, Centetodon pulcher, Stenacodon rarus, Antiacodon venustus, Bathrodon annectens, Bb. typus, Mesacodon spectosus, Hemiacodon gracilis, H. nanus, H. puciilus, Centetodon altidens, Hntomodon comptus, Entomacodon minutus, Centracodon delicatus, Nyctilestes serotinus, Ziphacodon rugatus, Harpalodon sylvestris, H. vulpinus, Orotherium uintanum, Helaletes boops, Paramys robustus, Tillomys senex, T. parvus, T. lucaris, Sciuravus ‘ parvidens, Colonymys celer, Apatemys bellus, A. bellulus, Entomaco- bea: A don angustidens, Triacodon grandis, T. nanus, EHuryacodon lepidus, Paleacodon vagus, Aletornis nobilis, A. pernix, A. venustus, A, bellus, A. gracilis, Uintornis lucaris, Thinosaurus agilis, T. crassus, T. grandis, T. leptodus, T. paucidens, Glyptosaurus princeps, Oreosaurus vagans, Tinosaurus stenodon, Glyptosaurus brevidens, G. rugosus, G. sphenodon, Oreosaurus lentus, O. gracilis, O. microdus, O. minutus , Tinosaurus lepidus, Iguanavus exilis, Tinoceras grandis, Dinoceras lacustris, and Oreocyon latidens. He described, from the Post- pliocene, near Bangor, Maine, Catarractes affinis, and from Monmouth county, New Jersey, Meleagris celer, and Grus proavus. Of the above list, it is stated by Cope thatthe new generic names are not generally defined. . Dr. Joseph Leidy* described, from the Bridger Group of Wyoming, Uintacyon edax, U. vorax, Chameleo pristinus, Lepidosteus atrox, L. notabilis, L. simplex, Amia gracilis, A. media, A. uintensis, Hypamia elegans, Pimelodus antiquus, Phareodus acutus, Hyrachyus nanus, Microsyops gracilis, Paleacodon verus, Hipposyus formosus, Paleo- syops junior, P. humilis, and Uintatherium robustum. © From the Niobrara Group, on the Niobrara river, in Nebraska, Felis angustus; from Green river, Oiigosomus grandevus; from the Black Foot country at the head of the Missouri, Tylosteus ornatus; - and from the Pliocene of Oregon, Hadrohyus supremus, Rhinoceros pacificus, and Stylemys oregonensis, Prof, F. B. Meek + described, from the Green River Group at Washakie, Wyoming, Unio washakiensis, and from Pacific Springs, Bythinella gregaria. T. A. Conrad{ described, from the Eocene of North Carolina, Ostre- nomia carolinensis ; and from the Miocene of the same state, Donazx idoneus. ee * Proc. Acad. Nat. Sci. + Geo. Sur. of Wyoming. t Proc. Acad. Nat. Sci. 100 Cincinnati Society of Natural History. In 1873, Prof. E. D. Cope* described, from the Bridger Group of Bitter creek, and Cottonwood creek; Limnohyus levidens; from a bluft on Green river, near the mouth of the Big Sandy, Wyoming, Palwosy- ops fontinalis; from the summit of Church Butte, Trionyx heteroglyp- tus;+ from the Bad Lands of Cottonwood creek, 7. scutumantiquum, Pappichthys plicatus, P. sclerops, P. levis, P. symphysis, Ehineastes radulus ; from Ham’s Fork, Bena ponderosa, Clastes anax ; from the Green River Group, near Evanston, Utah, Bathmodon latipes; from near Black Buttes, Hmys euthnetus, HL. megaulax, HL. pachylomus; from Upper Green river, Pappichthys corsoni, Rhineastes calvus, R. arcua- tus; from Green river basin,{ Antiacodon furcatus, now Sarcolemur Jurcatus, Orotherium (now Hyracotherium) index; from Cottonwood creek, Microsyops vicarius, Oligotomus cinctus ; from South Bitter creek, Paramys leptodus, Hobasileus galeatus, Achenodon insolens, from Henry’s Fork, Paleosyops diaconus, Hyruchyus implicatus; from near Evanston, Phenacodus primevus. He described, from the Miocene of Colorado.§ Hyopsodus mini- mus, Hypertragulus calcaratus, H. tricostatus, and Menotherium lemurinum; from the Miocene of the Western plains,|| Aelurodon mus- telimus, now Mustela parviloba, Aphelops megalodus, Paleolagus agapetilius,@ Colotaxis cristatus, Hyracodon quadriplicatus, now An- chisodon quadriplicatus, H. arcidens, Symborodon torvus, Miobasile- us ophryas, Megaceratops acer, M. helocerus, Peltosaurus granulosus, Testudo amphithorax, T. cultratus, 7. laticuneus, T. ligonitus, Domnina gradata,** Herpetotherium fugax, Daptophilus squalidens, Tomarctus brevirostris, Stibaru obtusilobus, Canis gregarius, Isacis (now Mio- dectes) caniculus, Paleolagus triplex, P. turgidus, Trictum avunculus, T. leporinum, T. paniense, Gymnoptychus minutus, G. nasutus, G. trilophus, Anchitherium cuneatum, and Trimerodus cedrensis, Prof. O. C. Marsht+ described, from the Eocene deposits of Wyoming and Oregon, Dinoceras mirabilis, Orohippus agilis, Colonoceras agres- tis, Dinoceras lucaris, Oreodon occidentalis, Rhinoceras’ annectens R. oregonensis, Tillotherium hyracoides ; from the Miocene of Colora- & Si eee * Proc. Am. Phil. Soc., vol. xili. + U.S. Geo. Sur., Wyoming, ete. t Pal. Bull. vol. xii. 2 Proc. Acad. Nat. Sci. | Pal. Bull. vol. xiv. q Pal. Bull. No. xv. ** Pal. Bull. No. xvi. 7+ Am. Jour. Sci. and Arts, 3d ser,, vol. v. Mesozoic and Cenozoic Geology and Paleontology. 101 do, Brontotherium gigas, and Hlotherium crassum; and from the Up- per Eocene of Wyoming,* Dinoceras laticeps. Dr. Joseph Leidy+ described, from the Bridger Group in the Buttes of Dry creek, Hyopsodus minusculus, Mysops fraternus, Washakius insignis, Saniva major ; from the Grizzly Buttes, Sinopa eximia ; from the Buttes, ten miles from Dry Creek Canon, Amia uintaensis; from the junction of Sand ‘and Green rivers, A. media; from Henry’s Fork, A. gracilis ; from Dry creek, Hypamia elegans ; from the junction of Big Sandy and Green rivers, Lepidosteus atrox, now Clastes atrox ; from Washakie station, LZ. simplex, L. notabilis, now Clastes notabilis ; from Big Sandy and Green rivers, Pimelodus antiquus, Phareodus acutus, Clupea alta, now Diplomystus altus; from the Miocene of Bridger creek, a tributary of John Day’s river, one of the branches of the Columbia, in Oregon, Dicotyles pristinus, Hlotherium imperator ; from Washington county, Texas, Anchitherium australe ; from Red Rock creek, a tributary of Jefferson Fork of the Missouri, Anchitherium agreste ; from Richmond, Virginia, Procamelus virginiensis, Tautoga conidens,{ Acipenser ornatus; from the Post-pliocene of California, Felis imperialis, and Auchenta hesterna.,. Prof. F. B. Meek§S described, from Church Buttes, Physa bridgeren- sis; from twelve miles south of Fort Bridger, Pupa leidyi; and from the upper beds exposed at Separation, on the U.P. R. R., Limnewa com- mactiles.. : Prof. Lesquereux described, from South Pare near Castello’s Ranch, Ophioglossum alleni, and Planera longifolia; from Elko station, Seq- uoia angustifolia, Thuya garmant, and Abies nevadensis. In 1874, Prof. E. D. Copel] described, from the Bridger Group of South Bitter creek, Hobasileus galeatus, and Achawnodon insolens ; from:the Miocene of Colorado, Symborodon hypoceras, Anchitherium exoletum, and Hippotherium paniense. Hedescribed from the Eocene of the Middle and South Parks, Colorado,4]. Amyzon commune, and Clupea theta, now Diplomystus thetus; from the White River Group, Hypertragulus tricostatus, Hlotherium ramosum, now Peionax ram- osus, and Menotherium Jemurinum ; from the Loup Fork Group, * Am. Jour. Sci. and Arts, 3d ser., vol. vi. + Cont. to Ext. Vert. Fauna, W. Terr. t Proc. Acad. Nat. Sci. 2 6th Ann. Rep. U-. S. Geo. Sur. Terr. | 7th Ann. Rep. U.S. Geo. Sur. Terr. 7 Bull. U.S. Geo. Sur. Terr. ° 102 Cincinnati Society of Natural History. Protohippus sejunctus, Procamelus angustidens, P. heterodontus, and Merycodus gemmifer, now Blastomeryx gemmifer. He determined that the lacustrine deposit in the valley of the Rio Grande, called the Santa Fe marls, is of Pliocene age, and described* Martes nambianus, now Putorius nambianus, Cosoryx .ramosus, now Dicrocerus ramosus, C. teres, now D. teres, Hesperomys, loxodon, now Humys loxodon, Panolax sanctefidei, Cathartes umbrosus, now Vultur umbrosus, Mustodon productus, and Steneofiber pansus. Prof. O. C, Marsh} described, from the Eocene of Wyoming, Orohip- pus major, Stylinodon mirus, and Tillotherium latidens; from the Mi- ocene of Colorado, Brontotherium ingens; from Nebraska, Dakota and Oregon, Miohippus annectens, Anchitherium anceps, A. celer, Anchip- pus brevidens, and Elotherium bathrodon; and from Pliocene strata of the west, Pliohippus pernix, P. robustus, Protohippus avus, Morothe- rium gigas, and M, leptonyx. Prof. Leo Lesquereux described,{ from Elko, Nevada, Lycopodium prominens, Myrica partita, Quercus elkoana, Diospyros copeana, Sa- pindus coriaceus; from Middle Park, Salvinia cyclophylla, Ulmus tenuinervis, Sapindus angustifolius, Staphylea acuminata, Rhus dry- meja, R. haydeni, Pterocarya americana; from Green river, Lquise- tum wyomingense; from Florissant, South Park, Acorus affinis, Myrica copiana, Weinmannia rosefolia, Ilex subdenticulata, I. undulata, Paliurus florissanti, Cesalpinia linearis, Acacia septentrionalis. The Eocene§ is found in North Carolina, between the Neuse and the Cape Fear, and in limited outcrops throughout the triangular region be- tween Newbern, Goldsboro and Wilmington. It consists of a lght colored, consolidated marlite, as in the steep bluffs on the Neuse, 10 miles below Goldsboro, or of a shell conglomerate as seen about New- bern, and 8 or 10 miles up Trent river, or of a white calcareous sand- stone, more or less compacted, as on the Neuse near Goldsboro; or of a gray and hard limestone, as about Richlands in Onslow; or of a coarse conglomerate of worn shells, sharks’ teeth, and fragments of bones and stony pebbles, as in the upper part of Wilmington and at Rocky Point; or of a fine shaly infusorial clay, light gray to ash col- ored, as in Sampson county near Faison’s depot. The outliers show that the formation, though limited in thickness, had a great horizontal extent, and once extended quite into the hill country of the State, and * Proc. Acad. Nat: Sci. Phil. + Am. Jour. Sci. and Arts, 2d ser., vol. vii. 4 - $ 7th Ann. Rep. U. 8. Geo. Sur. Terr. 2 Geo. of N. Carolina, 1875. Mesozoic and Cenozoic Geology and Paleontology. 103 nearly 150 miles from the present coast line, and to an elevation of nearly 400 feet. The Miocene occurs in disconnected patches, in river bluffs and in ravines over the seaboard region, and extending from the shore and the western margins of the’sounds 50 to 75 miles inland. It consists of beds of clay, sand and marl, which are locally filled with shells from 2 to 8 feet, and ovcasionally 10 to 20 feet. Prof. Theo. B. Comstock* said the Green River Group is used to de- signate that portion of the fresh-water Tertiary strata which lies di- rectly above the coal group, and which is the present surface formation over a large portion of the Green river basin, north of Fort Bridger. The upper limit is not readily definable at present, the transition be- tween the beds of this and the overlying group being rather gradual, but the general character of the two formations, both lithologically and palzontologically, differs greatly. The Green river beds are mainly composed of a series of shales, marls, and harder calcareous strata, the latter especially containing quyntities of the remains of fresh- water forms of life, with laminated layers, literally filled with the re- mains of land plants of the Phenogamous series. The outline of the ancient lake-basin, in which these strata were deposited, is not fully determined, but there are indications that its eastern boundary was outside of the present limits of the Green river basin, and there is no room for doubt that the Uinta mountains, and the Wahsatch cbain, then, as now, towered above its surface. Northward it is equally clear that the Wind River Range formed the shore of the great lake, with probably more or less of gently sloping border during a portion of the era of Lower Eocene deposition. ,Uhe excessive erosion has exposed the beds over the route from Fort Bridger to near South Pass, and generally speaking, the rock contains a considerable portion of calcic carbonate, with an abundance of ferric oxide produced by decomposi- tion and oxidation. Gypsum and calcite of different varieties are abundant, frequently occurring as thin, papery seams between the rock-layers, at other times forming masses of considerable extent. Some of the layers are little more than a pure clay shale, while there are a few quite arenaceous beds and some compact limestones. The texture of the different beds is quite variable, but, in general, the streams which have cut their channels through them are walled by nearly vertical cliffs, and the buttes and benches for the most part have * Rep. of Reconnaissance of Yellowstone river andN. W. Wyoming. 104 Cincinnati Society of Natural History. quite precipitous sides. Numerous joints occur in many of the strata, particularly in the more compact kinds, and fine examples of concre- tionary structure or weathering are not rare. The tendency of the thick beds of marly sandstone on the banks of Green river, at the crossing, to weather spheroidally, is very noticeable, and this is repeat- ed in various degrees in the argillaceous and calcareous rocks as well. The Bridger Group, though succeeding the Green River Group, is closely related to it, for the transition from one to the other is not abrupt, either in the structure of the beds or their contents. The Group is exposed at the surface over a considerable extent of country, northward and eastward from Fort Bridger as far as Little Sandy river and beyond, forming the top layers of numerous isolated buttes, During this epoch it is probable that the land was covered with fresh water in a lake as large as in the previous era, if not more extensive. The beds are mainly composed of dull-colored, indurated clays, and arenaceous layers of considerable thickness, the latter usually brown- ish, or dull yellow or gray, often.with more or less of a concretionary structure. The clays are generally compacted, but they become dis- integrated upon exposure to the atmosphere, and readily yield to the eroding forces. Some thinner layers of more calcareous material, with silicious seams, often affording interesting concretions, are interspersed, but they are rather exceptional than otherwise. The Green river and Bridger Groups are readily distinguished by the effects produced by erosion. The former presenting nearly vertical cliffs, so that the i1m- pression in crossing the country where it forms the surface rocks is that of traveling over an ordinary plain with occasional descents, by a succession of terraces, to the narrow valleys of the streams. On the contrary, where it is concealed, or only occasionally capped by the © Bridger Group, the country is very irregular, often simulating the ‘“ Bad Lands,” the beds of the latter being eroded without complete de- nudation, so that they stand out in buttes, or rude architectural forms. The deposits in the Yellowstone Lake basin, and in the valley of the main river and its tributaries, which may be regarded as Pliocene, are mainly the sediments of an ancient lake, of which the present body of water is the representative on a much reduced scale. Beautiful and highly instructive sections of the old beach formations are exposed in the valleys of the streams, particularly in the lower valley of Pelican creek, and far down the Yellowstone river, where they become more complicated and more interesting. An examination of these shows that the lake formerly extended over a mych larger area, and that it ee 4 3 RES —. 4 é Mesozoic and Cenozoic Geology and Paleontology. 105 6 has held its place amid changes of great importance. It was during the latter portion of the Tertiary age that much of the volcanic ac- tivity took place which was so general over this portion of the country, though probably only the closing stages of the lava flows are repre- sented by the eruptive deposits of the Pliocene epoch. A section on the present lake shore, between Bluff Point and Steam Point, in de- scending order, is as follows: 1. Grass-covered soil passing gradually to loose sand, 2 feet. 2. Various sand, gravel,.and spring deposits with scattered irony concretions, 6 feet. . 3. White and dark lake sand, very thinly laminated with beach structure, and occasional irony layers, 5 feet. 4, About 15 feet of thinly laminated, blue-black clay, locally con- torted and beautifully cut by a small rill, emanating as a spring from - one of the irony layers in No. 3. The water is slightly chalybeate. Other sections show the same general features with more or less vari- ation. They represent the upper portion of the Pliocene series, de- posited toward the close of volcanic activity, hence the occasional beds of volcanic ejectamenta which were poured out into the lake, are main- ly composed of volcanic sand and the finer textured conglomerates, as may well be seen near Steamboat springs. As we descend the valley of the Yellowstone river, we find the lower members of the group well exposed, and the beds of unmodified non-molten material becoming more common, with increasing proportions of the molten or lava series, until the latter are almost universal, and doubtless represent an earlier period, though frequently largely concealed by tlhe subsequent spring deposits. Near the close of the Pliocene epoch, the internal fires had * so far died out that the igneous ejections were of fitful occurrence, and geysers, solfataras, fumaroles, etc., abounded to an almost incredible extent, giving rise to enormous deposits of siliceous and calcareous material, which has continued to be deposited with decreasing vigor until the present day. Prof. G. K. Gilbert* found a section of Tertiary on the east face of Sam Pitch Plateau, at Wales, Utah, 1,292 feet in thickness, another near the head of the main Sevier river, in Utah, 560 feet, and another — on the north fork of Virgin river, between Mountain Lakelet and Rockville, in Southern Utah, estimated at 3,000 feet. Prof. EK. D. Copet described the Puerco marls as in all probability * Geo. Sur. W. 100th Meridian, vol. iii. + Ann. Rep. Explr. and Sur., W. 100th Meridian App. L. L. 106 Cincinnati Society of Natural History. a lacustrine formation of Eocene age, though having examined an out- crop for forty miles, he discovered no fossil remains except fossil wood. He said the material is so easily transported that the drainage chan- nels are cut to a great depth, and the Puerco river becomes the recep- tacle of great quantities of slimy-looking mud. Its unctious appear- ance resembles, strongly, soft soap, hence the name Puerco, greasy. These soft marls cover a belt some miles in width, and continue at the. foot of another line of sandstone bluffs, which bound the immediate valley of the Puerco to a point eighteen miles below Nacimiento. This section of the Eocene strata in the region west of the Sierra Madre Range in New Mexico consists of green and black marls, which he named the Puerco Group, 500 feet; sandstone of the Wasatch Group 1,000 feet, and red and gray marls of the same group, 1,500 feet; mak- ing a total thickness of 3,000 feet. He described,* from the Eocene of New Mexico, Ambloctonus sin- osus, Prototomus secundarius, P. multicuspis, P. strenuus, Diacodon alticuspis, D. celatus, Pelycodus frugivorus, Pantolestes chacensis, Opisthotomus astutus, O. flagrans, Antiacodon mentalis, A. crassus, Hyrachyus singularis, Hyracotherium:tapirinum, H. angustidens, H, cuspidatum, Bathmodon ilatidens, B. cuspidatus, Diplocynodus sphenops, Crocodilus grypus, C. wheeleri, and Dermatemys (?) costilatus. He described,t+ from the Miocene of Cumberland county, New Jersey, Phasganodus gentryi, Sphyrenodus silovianus, and Agabelus porca- tus ; from Flower’s marl pit, Duplin county, North Carolina,{ Pristis attenuatus ; from Edgerton’s plantation, in Wayne county, Pnewma- tosteus nahunticus; trom Halifax county, Mesoteras kerrianus, and Delphinapterus orcinus. From the Loup Fork Group of New * Mexico,§ Pliauchenia humphreysana, P. vulcanorum, Hippotheri- um calamarium, and Aphelops jenezanus ; and from the Pliocene of the West, Canis ursinus. Prof O. C. Marsh] described, from the Eocene of Wyoming, Lemu- ravus distans, Tillotherium fodiens ; from Utah, Diceratherium ad- venum, Diplacodon elatus, Orohippus uintensis, and Agriocherus pumilus, From the Miocene bad lands of Nebraska, Laopithecus ro- bustus, Anisacodon montanus ; from the John Day river in Oregon, * Geo. Sur. W. 100th Meridian, Syst. Catal. of Vertebrata. + Proc. Am. Phil. Sci., vol. xiv. t Geo. of N. Carolina. 2 Proc. Acad. Nat. Sci. | Am. Jour. Sei. and Arts, 3d ser., vol. ix. Mesozoic and Cenozoic Geology and Paleontology. 107 where the beds have an estimated thickness of 5,000 feet, Diceratheri- um armatum, D. nanum, Thinohyus lentus, and 7. socialis. T. A. Conrad* described, from the Eocene at Wilmington, North Carolina, Terebratula demissirostra; and from Beaufort, Pecten ani- sopleura and P. carolinensis. | From the Miocene near Wilmington, and other places in North Car- olina, Liropecten carolinensis, Ostrea perlirata, Placunomia fragosa, Raeta alta, R. erecta, Abra bella, A. holmesi, Noetia protexta, N. filosa, Mercenaria carolinensis, Leptothyris parilis, Trachycardium bellum, Mysia carolinensis, Saxicava protecta, Turritella perexilis, 7. carolin- ensis, Fissurella carolinensis, Littorina carolinensis, Busycon kerri, B. amoenum, and B. concinnum; from Suffolk, Va., Zizyphus virginicus. W.H. Dalit described, from the Miocene at Cerros Island, California, Waldheimia.kennedyi; trom the Pliocene at San Diego, Chrysodomus diegoensis. And R.C.Stearns{ described, from the same strata, Opalia anomala, and O. varicostata. In 1876, Prof. J. W. Powell§ subdivided the Tertiary rocks of the plateau province of the west in ascending order, into the “ Bitter Creek Group,” which is synonymous with the Wasatch Group, and has a thickness of 5,000 feet. It is succeeded by the Lower Green River Group, consisting of shales, often bituminous; sandstones; carbonace- ous shales and lignitic coal near the base. Thickness, 800 feet. This group is well exposed along Green river, from Green River station southward for 10 miles; in many of the escarpments of the Quien Hornet mountain, and a few miles northeast from the head of Ver- milion canon; on Snake river, six miles above the northern foot of Junction mountain; and on the elevated ledges known as Pine Bluffs, near the sources of the eastern tributaries of Vermilion creek. The beds are all fresh water. The Upper Green River Group consists of sandstones, sometimes argillaceous limestones, carbonaceous shales and lignitic coal, near the middle and in the lower part massive or irregularly bedded sandstone, ferruginous. Unconformable by erosion with lower Group. Thickness, 500 feet. The plant beds of this group are well exposed to the north of Green _ River station, and between that point and Alkali stage station, in many gulches and canons; in the cuts of the Union Pacific Railroad * Geo. of N. Carolina. + Proc. Cal. Acad. Sci., vol. v. t Proc. Acad. Nat. Sci. Phil. 2 Geo- of Uinta Mountains. 108 Cincinnati Society of Natural History. between Green River station and Bryan and in the escarpments on either side of Henry’s Fork at many places. The Tower sandstone is well shown in the cliffs at Green River station, and in that vicinity and below the mouth of Currant creek. The Tower sandstone is laid down unconformably on the Lower Green River Group, the unconformity being represented by gentle valleys of erosion. The Bridger Group consists of Bad Land sandstones (chiefly green sands ) limestones, shells, marls, and concretionary and stratified flints. Thickness, 2,000 feet. It is well exposed in the vicinity of Fort Bridger, at Church Buttes, at Haystack mountain and in the Cameo mountains. An outlying patch is found north of the Dry mountains between Vermilion creek and Snake river. Unconformity with the beds of the Lower Green River Group may be seen in the vicinity of Carter station, but uncon- formity with the Upper Green River Group has not been observed. The two are separated, however, upon lithological grounds, though the plane of demarkation is obscure. The moss agates for which the re- gion about Fort Bridger has been noted are from irregular beds and aggregations of chalcedony in this Group. The Brown’s Park Group consists of sandstones, gravels, limestones, concretionary and stratified flints. Unconformable with all under- lying rocks. Thickness, 1,800 feet. It is well represented at Brown’s Park, in northeastern Utah, and in northwestern Colorado. About five miles above the confluence of Snake river with the Yampa, the beds may be seen resting unconformably against Carboniferous strata, and on going north they may be observed to rest unconformably with the Bridger Group. In Brown’s Park, it lies in a deep basin of erosion, the bottom and sides of which are composed of Uinta sandstone. This basin is in the very axis of the Uinta uplift. Its sandstones are Bad Land rocks of exceedingly fine texture. In some places there are extensive and _ir- regular aggregations of chalcedony. The Bishop’s Mt. Conglomerate, which is unconformable by plica; tion and erosion with underlying rocks. Thickness, 300 feet. It is found on the summits of Bishop and Quien Hornet mountains, and up- on various tables in the Uinta mountains. On the north side of Con- nor basin, at the head of Sheep creek, this conglomerate has a thickness of more than 1,000 feet. It is neither a marine nor lacustrine deposit. but a subeerial one. Prof. Powell says, witnessing on every hand the accumulation of such Pian. 7h Mesozoic and Cenozoic Geology and Paleontology. 109 gravels in valleys and over plains where mountains rise to higher alti- tudes on either side, and having in many cases actually seen the cliffs breaking down, and the gravels rolling out on the floods of a storm, I am not willing to disregard explanations so obvious, and so certain, for an extraordinary and more violent hypothesis. Irregular accumula- tions of clay, accumulations of sand, of gravels, and bowlders, having, in a general way, all the lithologic characteristics of “drift,” are very common in the Rocky mountain region, and in many cases their origin can be traced to ordinary atmospheric agencies acting on the adjacent hills and mountains; and no glaciers or icebergs are needed for their explanation. We learn from Dr. Hayden,* that on the high divide between the drainage of the Arkansas and South Platte rivers, there occur fresh- water lake deposits, having a thickness of 1,000 or 1,500 feet, and cov- ering an area of about 40 miles trom north to south, and 50 miles from east to west, or about 2,000 square miles, called by Dr. Hayden, in 1869, the “ Monument Creek Group,” from the fact that the atmo- spheric agents have carved out of the beds peculiar monuments or col- umns. He referred the deposits to Miocene or Pliocene age ; later, in 1873, Prof. Cope, from the evidence of the hind leg and foot of an Ar- tiodactyle, and a fragment of Megaceratops coloradoensis, referred the deposits on the Colorado divide, perhaps the same, to the age of the Miocene. The texture of the rocks is quite varied. The lowet portion is composed of rather massive beds of sand- stone, varying from a pudding-stone to a fine-grained sandstone, usu- ally of a light color, sometimes of a yellow or iron-rust, with their in- tercalations of arenaceous clay. In the distance, the whole group, in many localities, presents a chalky-white appearance. At the im- mediate base of the mountains, just south of the small lake on the di- vide, the rocks are variegated sandstones, brick-red, white and yellow, varying in texture from a fine sandstone to a pudding-stone, with all the signs of deposition in moving waters. Still farther north, on the divide proper, the beds jut against the granites, inclining not more than 3°, and are made up of a coarse aggregate of feldspar and quartz crystals, so that it resembles a very coarse granite. It is plain that the sediments of this group were derived very largely from the granitoid rocks. The sediments become finer and finer as they recede eastward from the foot of the mountains into the plains. * U.S. Geo. and Geogr. Sur. of Colorado and Adjacent Territory. 110 Cincinnati Society of Natural History. To the eastward of the line of the Denver and Rio Grande Railroad, the surface is cut up into more or less rectangular masses, with rather broad table-shaped summits, varying from 400 to 800 feet in height. The sides are often very steep, almost inaccessible. At a remote period in the past, the erosion has been very great, carving out by an almost inappreciably slow process, these broad valleys, leaving these buttes here and there, composed of horizontal beds, to aid in forming some conception of the amount of denudation which has taken place. It is not possible at the present time to estimate the original thickness of this group, but believe it to have been very much greater than the highest beds now existing would indicate. The summits of many of the buttes are capped with a greater or less thickness of a heautiful purplish trachyte, which must have ascended in the form of dikes from beneath, and flowed over the surface. Much of the trachyte is a-sort of breccia, composed of rather coarse sandstones, which must have been caught in the melted material. Itis quite evident that these outflows occurred during the existence of the lake, though ata late period. Dr. Hayden synchronized the age of this group with the upper portion of the White River Group far to the northward, and probably with the fresh-water deposits in the South Park. Lake basins have occupied a large part of the country from the Isthmus of Darien to the Arctic Circle. In many instances they were merely expansions of river valleys, like the greater number of the lake basins of the present time. During the later Cretaceous and early Tertiary periods, the western portion of the continent was covered with immense lakes, but during the Pliocene and the interval to modern time, thousands of small lakes, with a few of large size, were distributed over the great area west of the Mississippi, and the basins with their peculiar deposits are found in the parks, among the moun- tains, and along every important valley. Dr. Hayden believed there are evidences of glacial action and morainal deposits in the valley of the Upper Arkansas river, at eleva- tions of 9,000 feet and upward, and along both flanks of the Sawatch » mountains; but, he said that he observed no proof of any wide ex- tended drift-action, like that of the New England States, in the Rocky mountains, as the superficial deposits are all of local origin, and the source is limited to the drainage of the streams in which the deposits are found. For example, all the marls and coarser deposits- in the valley of the Upper Arkansas, have the same origin, and the forces that produced them were limited geographically to the drainage » “ Mesozoic and Cenozoic Geology and Paleontology. a of that stream. That not a fragment of rock had been transported even from so short a distance as beyond the drainage west of the ‘Sawatch, or east of the Park ranges. He placed the superficial de- posits in one great period, extending from the Pliocene up to the present time, because in the aggregate they afford no proof of any break in the order of time. In the valley of Roaring Fork in the Elk mountains, the morainal deposits are remarkable for their thickness. The surface is covered with huge bowlders, some angular, and others partially rounded. The terraces are very conspicuous, rising, in some instances, to 1,000 feet or more above the bed of the stream, and strewed over with huge bowlders. . None of the stray materials in any of the valleys or gorges seem to have been transported a very great distance, and never, under any circumstances, is there any drift or vlacial deposits from a neighboring drainage ; in other words, the loose material does not pass from one independent valley to another. So it is all over the Rocky mountain region. All the drift or Post- pliocene deposits are local. Prof. E. D. Cope* described, from the Eocene of New Mexico, the giant bird Diatryma gigantea; and from the Pliocene, phosphate beds of South Carolina, Cyclotomodon vagrans. Prof. 0. C. Marsh+ described, from the Eocene of the Rocky moun- tain region, Hohippus validus, EH. pernix, Parahyus vagus, Dromo- cyon vorax, Dryptodon crassus, and Coryphodon hamatus. Dr. Joseph Leidy{ described, from the Eocene of New Jersey, Wy- liobates fastigiatus, and M. jugosus; from the Pliocene beds of Ash- ley river, South Carolina, Belemnoziphius prorops, Choneziphius liops, C. trachops, Etoroziphius coelops, Proroztphius macraps, Myliobates magister, M. mordazx, and Proroziphius chonops. Prof. C. A. White§ described, from the Eocene at Bijou basin, 40 miles east of Denver, Colorada, Corbicula powelli, Mesodesma, bishopi, Phorus exoneratus ; from Crow creek, Melaniva larunda; from the West, Tulotoma thompsoni; from the Lower Green River Group, 8 miles below Green River station, Wyoming, Helix riparia ; from the Upper Green River Group, at Henry’s Fork and Alkali station, Unio shoshonensis, Succinea papillispira, Pupa incolaia, and P. arenula. Prof. F. B. Meek] described, from the White River Group, on Pinot’s creek, Limnewa shumardi. * Proc. Acad. Nat. Sci. j Am. Jour. Sci. and Arts, 3d ser., vols. xi and xii. _t Proce. Acad. Nat. Sci. 2 Geo. of Uinta Mountains. | Hayden’s U.S. Geo. Sur. Terr. 112 Cincinnati Society of Natural History. G. T. Bettany* described, from the Miocene of John Day’s river, Oregon, Merycocherus leidyi, and M. temporalis. J. A. Allen+ described, from the lead crevices and superficial strata of the lead region of Wisconsin, Iowa, and Illinois, of supposed Plio- cene age, Canis mississippiensis, and Cervus whitney?. Charles M. Wallace found flint implements in the stratified drift, near Richmond, Virginia, which he referred to Post-pliocene age. In 1877, Dr. F. M. Endlicht found the Puerco Group forming the lowest member of the Wasatch, and well developed in southern Colora- do. It was best observed on the Lower Animas, where it consists of 1,000 to 1,200 feet of variegated shales and marls. At the base, they are a maddy green, changing into yellow or almost blue. Farther up, pink, pale orange, lilac, and reddish colors predominate, varied by in- terstrata of white or light yellow. Thin beds of sandstone merely of local occurrenee, however, separate these beds; not forming definite recognizable horizons. Farther east, these variegated marls gradual- ly change into shales and sandstones, so that they are no longer characteristic. Above them there occur 1,000 feet of yellow to brown sandstones and shales. Asa rule the beds of sandstone are heavy, weathering massively, but they frequently show but small thickness, and are interstratified with yellow and grayish shales. In some of the shales, indications of coal may be observed, but nowhere throughout the San Juan region was any vein found that would have been sufficiently large, or of good quality to be worked. : All the lower canons of the San Juan drainage, and that of the river - itself, are formed by this series of sandstones, and others superin- cumbent. Over the entire region which they cover, they are uniform, both in occurrence and in lithological character. Their very small dip to the south, 2° to 4°, and their total thickness of 3,000 feet, en- ables them to extend over a large area of country. Dr. B. F. Mudge found the Pliocene strata of Kansas resting direct- ly upon the Cretaceous. The material of the Pliocene deposits con- sists of sandstone of various shades of gray and brown, occasionally whitened by a small admixture of lime. The lower strata are usually composed of finer sand than the upper, and much more loose and friable in their texture. The overlying beds are of coarser ingredients, consisting of water-worn pebbles of metamorphic rocks, quartz, green- * Quar. Jour. Geo. Soc. Lond., vol. xxxii. + Am. Jour. Sci. and Arts, 3d ser., vol. xi. t 9th Ann. Rep. U.S. Geo. Sur. Terr. a ee Nis : . ie J = 7 / F nH ; Mesozoic aad Cenozoic Geology and Paleontology. 1138 stone, granite, syenite, and sometimes fragments of fossil wood from an older formation. These portions of the deposit, when crumbled, and the finer parts washed away, have much the appearance of drift, and have been mistaken for it. At Breadbowl Mound, Phillips county, it is about 200 feet above Deer creek, and at Sugarloaf Mound, in the western part of Rooks county, it is about 300 feet above the Solomon river. On Prairie Dog creek, in Norton county, it is 400 feet in thickness, and in the extreme northwestern part of the State it is still thicker. The formation like all the rest in the State, appears to dip slightly to the northwest. In the southern portion of the Pliocene, in the vicinity of Fort Wallace and Sheridan, the hill-tops are covered with a stratum about eight feet in thickness, very hard and siliceous. The material varies from coarse flint-quartz to chalcedony. The latter mineral shades from milk white to transparent, sometimes presenting a semiopal ap- pearance. The so-called moss agate is found in the upper few inches of the stratum. ‘This cap rock is interesting to the mineralogist by showing the moss agate in its various stages of formation. The lower portion of the eight feet indicates an imperfect chemical solution of the silica and black oxide of manganese, therefore the crystalization of the latter is imperfect. As we examine the strata from the bottom to the top, we find the chemical conditions more favorable and com- plete, so that the distinct quartz, chalcedony, and manganese of the bottom become more commingled toward the upper inch or half inch, where the silica must have been sufliciently fluid to allow the man- ganese to assume the form of sprig crystals. This peculiar deposit is common on all the high hill-tops of Wallace county. In King’s Geo. Sur.,* the Tertiary is divided into Eocene, Miocene, and Pliocene, each of which is again sub-divided in ascending order as follows. Kocene—1. Vermillion Creek Group ; 2. Green River Group; 3. Bridger Group ; 4. Uinta Group. Miocene-—1. White River Group; 2. Truckee Group. Pliocene—1. North Park Group; 2. Humboldt Group ; 3. Niobrara Group ; 4. Wyoming Conglomerate. The “ Ver- million Creek Group,” is a synonym of the Wasatch, and the “ Uinta Group,” of the Brown’s Park Group, and worse than all, the ‘‘ Niobrara Group” was a pre-occupied name for a Cretaceous Group. S. F. Emmons estimated the Eocene of the Green river basin at 7,500 feet in thickness. The beds of the Wasatch series, which are * Geo. Sur., 40th Parallel. ~ 114 Cincinnati Soctety of Natural History. chiefly arenaceous, were deposited in greater thickness than either of the other groups, and extended from the base of the Park range tu the flanks of the Wasatch mountains. The beds of the Green river series contrast with those of the other two groups by the relative prev-. alence of calcareous material, and the fineness of their sediments. They consist of a lower series of calcareous sandstones and impure limestones, containing some lignite seams, overlaid by a great thickness of re- markably fissile calcareous shales, abounding in remains of fish and insects, which reach an aggregate thickness of about 2,000 feet, and are characterized throughout by their prevailing white cvlor. The Bridger Group consists of a thickness of about 2,500 feet of arenaceous beds, with a small development of calcareous material, of a prevailing dull, greenish-gray color, characterized by the great quantity of verte- brate remains which have been buried in them. Its greatest develop- ment is in the southern portion of the Bridger basin. In the Washakie basin, on the western borders of the Little Muddy creek, and at Wash- akie mountain and Cathedral bluffs, the Wasatch series are exposed, weathering in castellated forms, and recognizable from great distances by their bright pinkish and reddish coloring. Washakie mountain and the line of bluffs which extend to Cathedral bluffs, are formed of beds of the Green river series in the upper portion, and with the red Wasatch beds at the base, the line of division can be distinctly traced, descending somewhat in horizon toward Barrel springs, and ascending again beyond toward Cathedral bluffs. A section taken at Sunny Point, near Little Snake river, gave a thickness from the river to the summit of the cliff of about 2,000 feet. The upper 950 feet belonging to the Green river series, and the remaining 1,050 feet to the Wasatch Group. The Green River Group is exposed in the valley of Brown’s Park, which is a bay-like depression, from 6 to 8 miles in width, occu- pying the geological axis of the eastern end of the Uinta mountains, from 1,000 to 1,200 feet in thickness. Throughout the valleys of the Little Snake and Yampa rivers, these groups have been worn into rounded ridges, where, generally, only disintegrated material is found. In the basin of Vermillion creek, the beds of the Wasatch Group have their greatest development. It was on one of the broad benches, be- tween the branches of this creek, to the east of Ruby Gulch, that the originators of the famous diamond fraud, of the summer of 1872, lo- cated their pretended discovery. An exposure of coarse, iron-stained sandstone, on the surface of the mesa, at the foot of Diamond Peak, was strewn by them with rough diamorfds and rubies, which were in- Mesozoic and Cenozoic Geology and Paleontology. 115 geniously mixed with the soil around, so as to make it appear that they came from the decomposition of the sandstone. Along Bear river, in Utah, from Bear River City to Evanston, the hills on either side are occupied by the nearly horizontal beds of the Wasatch Group. The greater part of Bear river plateau is covered with a considerable thickness of these beds, which are in general rather coarser and more conglomeratic than those of the Aspen plateau. Its summit varies in width from 2 to 4 miles, beyond which to the east- ward these beds are exposed in the deep canons of Woodruff, Randolph and Saleratus creeks, from 2,000 to 2,800 feet in thickness. He found the Savory plateau region covered, principally, by hori- zontal beds of the North Park Tertiary, which he referred to the Plio- cene, and which, as proved by exposures in the deeper cuts, on its northern edge, overlie the upturned edges of Cretaceous and earlier beds, while the higher portions of the ridges are capped by remnants of the Wyoming conglomerate. The best exposures are found in the open valleys at the heads of Savory and Jack’s creeks, and on the pass between the Archaean body of the Grand Encampment mountains and the Savory plateau. A thickness of not less than 1,000 feet of these beds is here exposed, which is made up in the upper portion of a thickness of about 300 feet of a drab, earthy, somewhat porous, lime- stone, sometimes inclosing small pebbles, underlaid by beds, which erade off insensibly from limy sandstones into coarse gravel beds. They occupy the valley ofthe North Platte to the South of Jack’s creek, forming long, gentle slopes, extending up from the river to the flanks of the Grand Encampment mountain, which, though so covered by recent deposits that only few exposures of the underlying Tertiary are found, sufficiently show the continuity of their original deposition. Their beds may be traced along the line of bluffs bordering the valley of Sage creek on the south and west. Here the upper member is a hard silicious shale, more like an older rock, under which are seen the white limy sandstones ; the lower beds being concealed beneath debris accumulations. Arnold Hague found the White River Group along the south and east face of Chalk bluffs, in Wyoming, resting unconformably upon the Laramie Group, and protruding from beneath the Pliocene beds. The strata are exposed near Carr’s station, on the Denver Pacific Railroad, eastward across Owl creek, the tributaries of Crow creek, and beyond. The thickness of the group is estimated at 300 feet, and is of Miocene age. 116 Cincinnati Society of Natural History. He estimated the thickness of this Pliocene lake strata, which he called the Niobrara Pliocene exposed in Wyoming, at from 1,200 to 1,500 feet. : The beds are found lying unconformably upon the older uplifted strata, and’ overlapping the area of the Miocene basin. South of the Union Pacific Railroad, they occur abutting against Mesozoic forma- tions; just north of Granite Canon, they lie next the Archaean mass ; and a short distance beyond, at the mouth of Crow Creek canon, are found essentially horizontal against nearly vertical Paleozoic lime- stones. From Crow creek, northward, they may be seen resting direct- ly upon every formation, from the Archean to the Fox Hills Group. The strata consists of marls, clays, coarse and fine sandstones, con- glomerates, with some nearly pure limestones. Fine, marly sand- stones are the predominant beds. | Overlying the Pliocene lake deposits on Sybille creek and its tribu- taries, and in the region of Chugwater and Pebble creeks, there occur beds of coarse and fine conglomerate, having a thickness of 300 or 400 feet. These beds have been called the Wyoming Conglomerate. In North Park, Pliocene beds lie unconformably upon the older rocks, resting in places against every formation from Archzean to the top of the Cretaceous, and are seen in undisturbed condition resting against the basalts. They extend over the entire Park basin, giving it the level, prairie-like aspect, which it presents from all the higher | elevations. He referred the Tertiary beds in the eroded basins and valleys worn out in the rhyolité in the Toyabe range of the Nevada basin, and noticable on Silver and Boone creeks to the Truckee Miocene. S. F. Emmons found the same formation in the valley of Reese river, near Ravenswood Peak, along the foot hills, both to the east and west of the Soldier’s Spring Valley basin, in the low depression of Indian valley, and in the re-entering bay north of Black Canon, with a thickness of over 700 feet. : The Truckee Miocene is so named from Truckee range, Nevada, which extends in a north and south line for 72 miles, and consists, for the greater part of the distance, of a single narrow ridge, barely more than 5 miles from base to base, but widening considerably at the southern end, where it is made up of broad fields of Tertiary eruptive rocks, Alfred R. C. Selwyn said* that between Blackwater and Stewart’s * Geo. Sur. of Canada. ee Mesozoic and Cenozoic Geology and Paleontology. 117 Lake, and thence to the Finlay Rapids, on Peace river, the country, with some exceptions, is more or less overspread with drift material ; much of this has been derived from the abrasion of the Tertiary for- mations, through which many of the principal valleys of the country have been cut, exposing alternating beds of clay, lignite, sand and rounded gravel, capped by vast sheets of volcanic products, chiefly porous and compact lavas—columnar and concretionary—and dense dolerite, forming high hills or undulating stony table-lands, such as that which is crossed by the wagon road between Clinton and Bridge creek, at an elevation of 4,000 or 5,000 feet. From Mr. Horetzky’s description of the abrupt character of the country on the Susqua river, and in the vicinity of Fort Stager on the Skeena, these Tertiary volcanic products are supposed to be extensively developed in that region. The lignite-Tertiary strata which are assumed to have pre- ceded the latest of these volcanic outbursts, occupy undefined, but ex- tensive areas between Fort George and McLeod’s lake ; and probably continue thence to the valley of Nation river, with only such. interrup- tions as are the result, partly, of the original unevenness of the sur- face upon which they were laid down, and partly of the subsequent de- nuding agencies to which they have been subjected, giving rise to out- croppings of the older rocks, either as hills or ridges rising above the general level of the country, or appearing as rocky bars or canons in the deep-cut channels of the rivers. The general similarity of some of the sands and gravels of the drift period to those of Tertiary age, makes it difficult, without close and critical examination of each ex- posure, to determine to which period they should be referred, and the distribution of the drift upon the Tertiary deposits is so irregular as to make it quite impracticable to define their respective limits. At about three miles below Nation river, a steep cliff rises on the right bank of Parsnip river, from the water’s edge to 70 or 80 feet. At the base, stiff blue clays are seen, and these are overlaid by layers of sand and fine gravel, passing at the top into coarse rounded gravel. This is, probably, near the northern limit of the Parsnip river lgnite- Tertiary basin, as a short distance further a rocky ridge crosses the river and crops out in both banks, the country then rising rapidly, on one side to the Rocky mountains, and on the other to the watershed between the Omineca and the Parsnip vivers. On the eastern side of the mountains there do not appear to be any deposits which can be re- ferred with certainity to the lignite-Tertiary series. At intervals along the river, on both sides, deposits of stratified sand and gravel, cut into 118 Cincinnati Society of Natural History. benches and terraces, extend from the water to elevations of seven or eight hundred feet. Somewhat similar sands and gravels are thinly — spread over many parts of the great prairie plateau, which stretches eastward from the base of the mountains. Europe. Chairman of Subsection of Chemistry—W. R. Nichols, Boston, Mass.. Chairman of Subsection of Microscopy—A.B. Hervey, Taunton, Mass. Chairman of Subsection of Anthropology—Garrick Mallery, Wash- ington, D. C. | Chairman of Subsection of Entomology—John G. Morris, of Balti- more, Md. Permanent Secretary—F. W. Putnam, Cambridge, Mass. General Secretary—C. V. Riley, Washington, D. C. Secretary of Section A—John Trowbridge, Cambridge, Mass. Secretary of Section B—William Saunders, London, Ontario. Secretary of Subsection of Chemistry—H. W. Wiley, Lafayette, Ind. Secretary of Subsection of Microscopy—sS. P. Sharples, Boston, Mass: Secretary of Subsection of Anthropology—J. G. Henderson, Win- chester, Ill. Secretary of Subsection of Entomology—B. P. Mann, Cambridge, Mass. Treasurer—William 8. Vaux, Philadelphia, Pa. The officers of the Local Committee are, Hon. A. T. Goshorn, Chair- man; Mr. Julius Dexter, Treasurer; and Profs. F. W. Clarke and Or- mond Stone, Secretaries. Committee on Reception, Hon. J. D. Cox, Chairman; Miss E. O. Abbot, Mrs. Robt. Brown, Jr., Mrs. William Dodd, Mrs. T. J. Emery, Miss Fannie Field, Mrs. Richard Folsom, Mrs. M. F. Force, Mrs. G. R. Fries, Miss Emma Goepper, Mrs. Z. M. Humphrey, Mrs. John Kebler, Miss Annie Laws, Mrs. T. D. Lincoln, Mrs. M. L. Nichols, Mrs. A. F.’ Perry, Mrs. R. S. Rust, Mrs. H. C. Whitman, and Mrs, A. E. Wilde, assisted by 131 gentlemen. Committee of twelve on Finance, Julius Dexter, Chairman. Committee of twelve on Rooms, William McAlpin, Chairman. Committee of nine on Hotels, Herbert Jenney, Chairman. Committee on Entertainments and Excursions, George W. Jones, Chairman, Mrs. John Davis, Mrs. W. B. Davis, Mrs. Wm. H. Davis, Mrs. A. J. Howe, Mrs. John Kilgour, Mrs. Alphonso Taft, and Mrs. Elkanah Williams, assisted by 18 gentlemen. Committee of eight on Transportation, W. L. O’Brien, Chairman. Committee of thirteen on Press and Printing, Archer Brown, Chair- — man. ; THE JOURNAL INT WLTY TURAL STIR PROCEEDINGS OF THE SOCTETY. Turspay Evenine, July 2, 1881. Dr. R. M. Byrnes, President, in the chair. Present, 18 members. F S. A. Miller, read part of a paper, entitled “Observations on the _ Unification of Geological Nomenclature, with special reference to the Silurian formation of North America,” which he had prepared to be read before the International Geological Congress, which assembled, in September, at Bologna, Italy. Donations were announced as follows : | From Messrs. Ellison, four species of bird-skins, and two specimens of bryozoans ; from Robert Clarke, 60 species marine algee—named ,; from G. Holterhoff, jr., forty-one species of native birds’ eggs, and ninety species of land shells; from Davis L. James, nine species of seeds ; from Dr. Bronson, one bottle of ashes from a mound in West Virginia, and a viviparous fish from California ; from J. F. James, a tree-frog, and the skull of a crow; from Kittredge & Co., the U. 8. Business Directory for 1878 ; from J. H. & B. M, Seaman, a section of _ wooden water-main from the streets of Cincinnati—supposed date 1815; trom Captain A. H. Bugher, through Dr. A. E. Heighway, a magnificent starfish from Florida; from Dr. A. E. Heighway, a fine specimen of Peterygotus bilobus, from Buffalo, N. Y.; from W. C. Egan, Chicago, Ill., Saccocrinusmarcouanus, 8. necis, S. infelix, Melocrinus obpyra- 182 Cincinnati Society of Natural History. midalis, Ichthyocrinus corbis, of Winchell and Marcy, recently re- described by 8. A. Miller ; from James R. Challen, fine specimens of gold-bearing quartz, from Georgia ; from Professor J. W. Hall, jr., a specimen of Cutenia syrtalis, in alcohol. By exchange, casts of the horns of two extinct bovine animals, viz: Bos primigenius, and Ovibos cavifrons, the former from Arkansas, the latter from Italy. } Turspay Evernine, August 2, 1881. Dr. R. M. Byrnes, President, in the chair. Present, 15 members. Mr. Joseph F. James read a paper upon the “Century Plant,” and Prof. G. W. Harper made some remarks upon land shells and his new species Patula bryanti. James W. Abert, of Newport, Kentucky, was elected to membership. Donations were announced as follows : From B. Kittredge & Co., four volumes of books ; from Dr. W. H. Mussey, a curious quartz crystal, from Arkansas; from Dr. J. A. Warder, a pamphlet ; from the Smithsonian Institution, ‘‘ The Proceed- ings of the U.S. National Museum for 1880 ;,” from U. P. James, Esq., 65 species of Cincinnati fossils, described by himself; from Joseph Foster, jr., 6 specimens of polished marble ; from D. M. Stewart, Esq., 9 specimens of steatite ; from E. Mills, Esq., 160 species of lepidoptera; and from Prof. G. W. Harper 5 arrow-heads, from North Carolina. Turspay Evenine, September 2, 1881. This evening only seven members including the President were present, and this number being less than a quorum, no business was transacted. The excessive heat, and the fact that the members had attended so many scientific meetings of the A., A. A. S. within the past — month, acted, no doubt, to prevent a quorum at this meeting. It is noted, however, as the first meeting within the past five years that failed for want of a quorum. ls nie ee Mesozoic aad Cenozoic Geology and Paleontology. 183 MESOZOIC AND C4INOZOIC GHOLOGY CONTINU ED— THE DRIFT OF THE CENTRAL PART OF THE CON- TINEN T. By 8. A. Mitier, Esq. | Continued from Vol. iv., page 144. | We now come to the consideration of the sand, gravel and bowlders constituting the drift of the central part of the continent; the scratches and furrows upon the rocks; the ancient soil beneath the drift ; and the animal and vegetable remains which immediately preceded the drift, and also such as are found within it. It is idle to talk of continental elevations or depressions, for the whole science of geology and paleontology teaches us of the gradual growth or formation of continents. The appearance of islands above water, until an archipelago is formed, followed by the slow filling up of the shallow places and the intermittent local elevation of mountain chains, through vast geological ages, until the islands are thoroughly united into one vast body or continent, is the history of all continental elevations, and science teaches us of none other, and if continents have been depressed they must now be beneath the ocean, for we know nothing of such phenomena. We have already seen the vast deposits of the Triassic and Jurassic periods, followed by the marine and brackish water deposits of the Cretaceous age that so well nigh formed the outlines of this continent. The elevation of the mountain chains that caused the formation of vast internal lakes, which have slowly drained themselves through all Tertiary time, and the slight elevation of some parts of the coast during the same period has given us the present form of our continent. As soon as an island appeared above the ocean the denudation of its surface, from atmospheric causes, began. The rains at once com- menced the excavation of valleys and ravines, and when the islands began to assume a continental shape, the valleys must necessarily have been correspondingly increased in size. As the Appalachian range dates back, in part, as far as the close of paleeozoic time, so the Ohio river and other streams from this mountain chain have the same age. Another drainage system existed from the Laurentian mountains by a way that has been interrupted and thrown into a series of lakes, but the ancient valley has been traced from Lake Huron through Lakes Erie and Ontario. To the west and north of IN OSS SNES eae MONEE CIAL Ne , ie - Me aM 184 Cincinnati Society of Natural History. this drainage system, vast internal lakes were formed by the elevation of the western mountain chains, which overflowed and drained them- selves across the central part of the continent, and produced, as we will see, in the sequel, all the phenomena of the drift. As heretofore, we will follow the historical and chronological order _ of discovery as far as practicable. In 1817, Dr. Daniel Drake,* of Cincinnati, wrote an essay upon the alluvial and drift formations of Ohio and the surrounding country. The letter was not published, however, until 1825. He supposed that the gravel and sand which spreads itself over the western part of Ohio, and is not found over eastern Kentucky, is the result of an inundation, having its origin north of the lakes, and that the large bowlders and blocks of stone, distributed over the country, were transported by large fields of ice and icebergs, which floated from the arctic regions during this inundation. He said, the ice to which they were attached could not of course pass a certain latitude ; and from the great increase of these masses as we advance toward the north, it would seem that many of the icebergs suffered dissolution long before they arrived at this locality. In 1820, Caleb Atwater} stated, that an arrow-head was found in the alluvium, when digging a well at Cincinnati, 90 feet below the sur- face ; that a human skeleton was found in the alluvium at Pickaway plains, 173 feet below the surface, that could not have been interred by human hands in that position ; and he figured and described a human skull of a very low grade, which was found nine feet below the surface, in such a position as to suggest its contemporaneity with the drift era. : | In 1825, Sayers Gazley{ found fossil wood in Hamilton county, Ohio, below the gravel, and intermixed with it and bluish earth, at depths from 10 to 40 feet below the surface, and apparently where the trees had originally grown. In 1838, Prof. James Hall§ observed the indications of diluvial action, in western New York, in the accumulations of gravel, sand, pebbles and bowlders of all dimensions strewn over the surface. In some places slight scratches were observed on the rocks, while in others they were numerous and deep, often extending for several feet, and in * Trans. Am. Phil. Soe., vol. ii. + Am. Jour. Sci. and Arts. t Ibid. 2 Geo. Rep. N. Y. Mesozoic and Cenozoic Geology and Paleontology. 185 one case a continuous furrow was found 100 feet in length. The general direction of these scratches is N.N.E. and S.8.W. though they vary a little. One of the remarkable features of the country is a *‘ Lake ridge” passing through the four lake counties nearly parallel to the lake shore, and from four to eight miles distant from the lake, The width of the ridge at the base is from four to eight rods, and narrow- ing toward the top to only two or three rods in width. In many places it much exceeds this width, The elevation of this ridge above lake Ontario is from 160 to 200 feet, though it varies a little from this at some places. The whole of the ridge is superficial, being composed of sand, gravel and pebbles, in all respects similar to those forming the beaches along the present lakeshore. South of the ridge there are numerous parallel ridges, composed of sand and gravel, rising about 25 to 35 feet above the general level, and having uniformly a north and south direction, but never crossing the lake ridge. The opinion ex- pressed in relation to this ridge is that it once constituted part of the shore of the lake, and consequently that the water in the lake was once 160 or 200 feet higher than at present, and that the north and south ridges resulted from the overflow of the lake and the pouring out of its waters in a southerly direction. Prof. J. W. Foster* separated the surface deposits of Central Ohio into: 1. Vegetable mold; 2. Loam, or a mixture of sand and clay; 3. Sand and pebbles; 4. Yellow clay; 5, Dark blue clay effervescing with acids. The whole of which has a thickness of from 950 to 150 feet. And also over the surface of the country there are scattered bowlders of granite, syenite, quartz, etc. In the region about Columbus, some of these erratic blocks contain 1,000 cubic feet. Not even a primitive pebble has been found on the highlands east of Zanesville, showing that the valley of the Muskingum formed a connection of the currents of water, that swept over the country, with the Ohio river. He de- scribed from an excavation for the canal at Nashport, Ohio, Casto- roides ohioensis. It was taken from a layer of dark carbonaceous silt, below a yellowish clay bed 14 feet in thickness, but above a layer of pebbles of primitive rocks and the blue clay at the bottom ofthe canal. Prof. John Locke found the surface of the rocks at Light’s quarry seven miles above Dayton, about 448 feet above the Ohio river at Cin- cinnati, planed, scratched and grooved. The quarry had _ been stripped of soil, more or less, over ten acres. The natural surface of the stone is very rough, and in some places this roughness was un- * Ohio Geo. Rep. 1838. pia Cg 5 > ae Se ate © s Neyisia eee ae ee ee Pa 186 Cincinnati Society of Natural History. touched, in others the prominences were just touched by the grinding operation, partially worn down, or entirely obliterated, leaving a flat, but unpolished surface, and in many other places the surface is polished, and grooved. The grooves are, in width, from lines scarcely visible, to those three fourths of an inch wide, and from one fortieth to. one eighth of an inch deep, and traverse the quarry from between N. 19° to N. 33° west, to the opposite points, in lines exactly straight, and in fassicles of sometimes 10 in number, exactly parallel, cleanly en- graved in compact limestone, without seam or fault of any kind, and in a surface ground down to a perfect plane. The grooves appear as if they had been formed by icebergs floating over the terrace, which ‘is the highest in the neighborhood, and dragging gravel and bowlders frozen into its lower surface, over the plane of the stone. In 1842, Lardner Vanuxem* found the drift scratches in Central New York confined to no particular rock, and at no particular elevation, but not uncommon, and corresponding, in direction, with the course of the valley, or of the valleys in which they occur. One of the best localities for observing the phenomena is at a quarry two and a half miles northeast of Amsterdam. The surface of the rock is covy- ered with soil and earth, which, when removed, shows a water-worn sur- face with two or three sets of scratches, exhibiting great regularity, and — having a common direction toward the east, one set of which is about eight degrees south. The scratches, including furrows, are generally from a mere line to one fourth of an inch wide, and from one to two tenths of an inch and more in depth. Some of them show that the moving power which produced them, passed over the sarias with a vibratory or tremulous motion. In 18438, Prof. James Hall} said that the northern part of the fourth district of New York, and the low slopes and deeper valleys of the southern part, are covered to a greater or less depth by superficial materials of more northern origin, mingled with those of the rock on which the deposit rests. All the formations have suffered greatly from denudation, and the abraded fragments of each constitute a large proportion of the superficial detritus resting on its southern neighbor. The size of the fragments always bears a proportion to the distance they have been transported from the parent rock. Often, a huge mass of a northern rock rests upon the margin of the one next south of it, while at a distance of 10 or 20 miles farther south, only small * Geo. 3d Dist., N. Y. + Geo. Sur. 4th Dist., N. Y. par : Go tae Mesozoic and Cenozoic Geology and Paleontology. 187 pebbles of the same occur. In some places the coarser and _ finer materials are intermingled, in the greatest confusion, and heaped up into conical hills thickly scattered over the surface. And again the same materials are accumulated in long hills or ridges having a deter- minate direction, and sloping down from a high northern elevation to the general level of the country south. On one hand, we have comparatively an evenly distributed deposit, as if made by the retiring waters of an ocean; on the other, the long hills, with certain directions, show a determinate course and more powerful current in the ocean, while the irregular, conical and dome- shaped hills, with deep, bowl-shaped cavities, show the force of con- tending currents, or of other obstructions, in the course of the trans- ported materials. The great bulk of the deposit, whether evenly distributed or irregu- larly raised into hills and ridges, is composed of the rock but a short distance on the north, or perhaps of the one on which it rests, with a constantly decreasing proportion of rocks of northern origin. The ‘materials of the primary rocks constitute but a comparatively small proportion of the superficial accumulations of western New York. The local origin of the drift is shown by the sections everywhere examined. A section on Irondequoit bay, is as follows: 1. Medina sandstone, shaly with bands of green. 2. Fragments and rolled masses of the sandstone below, with gravel and sand; this contains a few pebbles of the shaly, calcareous sandstone next on the north. 3. Bed of fine sand. 4. Stratum of sandstone pebbies, cemented into a conglomer- ate by oxide of iron and carbonate of lime. 5. Stratum of pebbles and sand. 6. A course deposit of pebbles of the Medina sandstone below, with gravel und sand. 7. The soil of sandy loam. An- other section 70 miles farther west on the bank of lake Ontario, at the town of Wilson, in Niagara county, is as follows: 1. Red clay and gravel of the Medina sandstone. 2. Blue clay and gravel. The pebbles are principally of the rocks of the Hudson River Group. 3. Gravel, clay and sand, of the neighboring ‘rocks, folding over and passing beneath No, 2. 4. The soil of clayey loam with clay below. The sections of the drift almost universally correspond with these, and their explanation, viz: a bed of broken fragments, with worn pebbles resting upon the rock from which they are derived. The granite and other materials of a far northern origin rarely constituting apart. And where they do form a part, the deposit may have under- gone some subsequent change. 188 Cincinnati Society of Natural History. Grooves or strize are found upon the surface of all the rocks beneath the drift in the fourth district, which are of sufficient hardness to re- ceive and retain such impressions. From the Medina sandstone, at the level of lake Ontario, to the summit of the Carboniferous conglomer- ate, in the southern part of the State, some of the strata in every group bear upon their surface these markings of former abrasion, -and evidence of moving force. The direction of these strize vary but few degrees from N. 35° E. and 8, 35° W. in their general course. Short and shallow strie are abundant, which vary ten and fifteen degrees from this direction, but these have no continuous course, and apparent- ly fall into the main direction after a few feet. These markings range from the slightest possible scratch, to grooves of half an inch in width and one fourth of an inch in depth. The grooves seem to have been made by a hard substance, moved with great force and under great. pressure, for fragments are found broken out as the grooves approach a fissure in the strata, as if crushed out by some heavy body, and some- times the grooves are observed following, somewhat obliquely, the fractured slope. The outcropping edges of strata, previously polished and grooved, are often found overturned, upon the rock, in place. At Rochester, the surface of the limestone is finely striated, and al- most perfectly polished by the abrading force. The material here rest- ing upon the rock is fine sandy loam; in another locality a mile farther south, it is covered by coarse limestone gravel and sandstone pebbles, with bowlders of granite. The striz here are N.N.E. and $.S.W. At Black Rock, the surface of the Corniferous limestone shows that the nodules of hornstone interrupted the progress of the striz and stand above the surrounding polished surface. The direction here is N. 15° E. and 8. 35° W. At the cliff of Lake Erie in Portland, Chautauqua county, the rocky strata below have been uplifted, broken and con- torted; the fragments intermingled with clay and gravel, and the same pressed beneath the strata, which otherwise appear to be in place. The terrace at Lewiston is formed by the upper part of the Medina sandstone, the Clinton Group and the Niagara shale, capped by about twenty feet of Niagara limestone. The top of this terrace is 350 feet above Lake Ontario, and more than 200 feet above the plain about Lewiston. The Niagara shale is carried away so as to leave the lime- stone of the Clinton Group torming a projecting shelf about 100 feet below the top of the terrace. The surface of this projecting shelf is deeply grooved and striated, the grooves having a general southern tendency, but more irregular than where they are seen upon the lime- vt Read Ay had 7 oe see. Le Mesozoic and Cenozoic Geology and Paleontology. 189 stone on the top of the terrace; and at this place, the surfaces 200 feet lower, and 100 feet higher, are scored in like manner, What agency could produce this effect ? Here is an abrupt elevation of 100 feet above the striated surface; and it seems hardly possible that an island of ice, loaded with granite bowlders, could have stranded upon this pro- jecting shelf, and produced the scoring, and that, at the same time, others above and below could be made in like manner. The fourth district, in its greatest elevation ofabout 2,000 feet above tide water, descends to the level of Lake Ontario, 240 feet above tide, ' for the most part, ina series of steps or terraces over the successive formations; the surfaces of these, frum the highest to the lowest, are grooved and striated, and in the limestones often beautifully polished. There is no high land on the north, from which glaciers could origin- ate to cover this entire surface. The relative levels, as well as the directions of the water courses, must also have been different, to have allowed of such effects from glaciers; for, under present circumstances, we should hardly expect to find a glacier advancing from the valley of Lake Ontario, toward the southern margin of the State, and ascending nearly 2,000 feet in 100 miles. Even admitting the glacial theory to - be true, it is probable that the glaciers would originate among the mountains of Canada, or farther north among the primary rocks; and in this event, we might expect to meet, intermingled with the earliest drift, a considerable proportion of granite and other pebbles and bowlders of the older rocks, which is not the case. There is another fact worthy of notice. The vertical faces of joints, when much separated and nearly coinciding with the direction of these grooves, are polished in the same manner as the surfaces. Thechinks and fissures, in the harder rocks along the sea shore, are polished, in like manner, by the washing in of sand and pebbles by the advancing and retiring waves. The first plateau above Lake Ontario is often plentifully covered with bowlders. These usually lie upon the surface, and always upon the top of the drift. They are not evenly distributed, but often appear in immense numbers, scattered over several acres; while beyond this, for a great distance, few are to be found. There appears to be no law regulating their distribution, though they are more abundant in the eastern than in the western part of the district. The bowlders are often in immense numbers on the low ground just north of the Ridge road from Wayne county to the Niagara river, and appear as if they had been brought there while the water was limited by this barrier, 190 Cincinnati Society of Natural History. and spread over the bottom in shallow water near theshore. In higher situations, and just beneath the great limestone terrace they again ap- pear in abundance, as if this elevation prevented their farther advance to the south. The bowlders are most abundant in Wayne and the eastern part of Monroe county; going westward from the Genesee they are less so, becoming extremely rare in Erie and Niagara counties, As we ascend the second limestone terrace formed by the Helderberg range of limestones extending westward, bowlders become perceptibly less numerous; they are irregularly scattered, and at few points pre- sent the thickly covered fields which are observed farther north. Very few ascend the slope formed by the passage of the Hamilton Group to the rocks above; and in all the previous cases, they seem to have been brought on, at intervals, in great numbers, and their limits bounded by the different elevations of the surface. As we pass southward over the higher groups, bowlders become exceedingly rare; and finally toward the southern margin of the State they are rarely seen. Some of them bear evidence of much wearing, heing actually striated upon the surface, and sometimes flattened on one side, as if held in that position while moved over a bottom of gravel or sand resting up- on the strata beneath. For the most part, however, they bear no eyvi- dence of attrition beyond what similar masses do a few miles from their parent rock, and thus offer no argument for their mode of trans- portation. Many of them are angular, and with no appearance of at- trition beyond what the weathering in their present situations would produce. The process by which fragments of granite become rounded bowlders, is illustrated by the desquamation which takes place in some granites, the weathering in place, and the attrition in mountain streams soon after leaving their native beds. A large proportion of the bowl- ders of western New York are of dark felspathic granite and red gran - ites like those of the northern part of the State. Some other varieties occur, which are likewise referable to the same region. A few of crys- talline limestone with serpentine, and a few of specular iron ore have been found which are like rock found in St. Lawrence county. In many places, the drift hills have no definite direction, but those north of the great valleys of Seneca and Cayuga lakes are long ele- vated ridges, rising abruptly on the north, to a height of 50 or 60 feet, and sloping gradually down to their southern termination. The form of the hills is precisely such as would be made by a powerful current passing southward through these valleys, piling up the coarser ma- terials at the northern extremity, and moving the finer ones farther on, a eee te ee ae ee, cn eS ‘ : a i ] t Mesozoic and Cenozoic Geology and Paleontology. 191 until'they were in some measure protected by this barrier before they were deposited. One of the most interesting of the superficial deposits is the Lake ridge, which, from Sodus in Wayne county, with some trifling excep- tions, is a traveled highway nearly as far as the Niagara river. Be- yond this it can be traced to the head of Lake Ontario. It follows the general course of the Lake; being at its nearest point about three miles distant, and at its greatest about eight miles. In some places it is strongly defined, descending toward the lake twenty or thirty and even fifty feet in a moderate slope. It consists of sand and gravel, and contains fragments of wood and shells, and in every respect it re sembles the sea beaches. It was undvuubtedly the ancient beach of Lake Ontario, or a body of water which once stood at this elevation. ~The top of the lake ridge is 158 feet above Lake Ontario at Lockport ; 185 feet at Middleport, and 188 feet at Albion and Brockport. Beside this well-defined ridge or ancient beach there are a number of less distinctly defined terraces of gravel and sand at much higher elevations, on the hill sides, leading to the supposition that the water of the Lake stood more than 750 feet higher than at present, or that the country has been correspondingly depressed. Prof. W. W. Mather* found that the drift scratches, grooves and fur- rows conform in their directions to those in whicb currents would flow, if the country were mostly covered by water. In some parts, they cor- respond in direction to the main water-sheds ; in others they do not, but where they do not, the deviation is owing to some topographical feature which disturbed the course of the currents of water. In 1845, Alexander Murray} found the drift of western Canada, con- sisting of various beds of clay, sand and gravel, interspersed with large bowlders. The thickness frequently reaches 200 or 300 feet. The clay cliffs of Scarborough, are 320 feet. The ridges running parallel to the north shore of Lake Ontario, are 200 or 300 feet, and the high- lands in Oxford, are 100 or 200 feet, and even more, and the banks of Grand river often expose a considerable amount of drift. The southern shores of lake Simcoe, are extensive sandy plains, which are in many places thickly strewed with bowlders, and bear proof of having once been the bottom ofthe lake. Wherever gravel is found, its pebbles consist of limestone, and with the larger fragments of that formation, they con- tain the fossils of the calcareous strata at Rama on the north, The * Geo. of the lst Geological Dist., N. Y. + Geo. Sur. of Canada. id rE iS el eae Tbk iL 2 oan ‘ ‘. ON OE ee i Ce ee rT 192 : Cincinnati Society of Natural History. whole formation consists of the disintegrated rocks of the immediate locality, or those at no great distance north. The grooves and scratches upon the rocks between Niagara and Hamilton, have a north and south direction. In 1847, W. KE. Logan* found on the north shore of Lake Superior, about three miles below the Petits Ecrits, six terraces, in addition to the summit, which, presenting a level surface throughout the whole length, may be considered a seventh. Blocking up the extremity of a deep cone from the rock on one side to that on the other, the accumu- lation is a barrier to an extensive flat and marshy surface, that spreads out in a valley behind, down to the level of which there is a rapid slope from the summit of the drift, at a distance of about 1,000 yards from the margin of the lake. The height of the ancient beaches as measured by a pocket spirit-level is as follows: Above the Lake. Above the Sea. Feet. F ee eet. Beste. ES yo. hie Goel ave, oo. 4s ale ee 30 627 Lol OG aaa eae MR eee tone nee SE LS ER AC 40 637 EXCL 1 RE aaah eran iC AN oi epred Mec Airey cai ls 90 687 Ppp 07 8 cl Ode oie eek RN Re 224 821 Bila» © sated Seater ae J Sid i as 259 856 I oh oe. re as iy aes eo, ne re 267 864 fit > OT SUMMIG. noe eee Ce ee 331 928 The 3d and 4th beaches are the most decidedly marked, the steps, rising behind them, sloping up at an angle of nearly 30°. Alexander Murrayt+ described the drift on the Kamanitiquia river, which flows into Lake Superior, near Fort William, as consisting be- tween McKay’s mountain and the Grand Falls, where the principal display was found, of a light buff-colored clay, covered over by strati- fied yellow ferruginous sand, both together attaining a thickness of 60 feet above the level of the water. Banks of sand were found on Dog river, at a much higher level than the deposit further down. In 1848, John L. Leconte{ described, from a Post-pliocene deposit in acrevice in northern Illinois, Platygonus compressus and Anomo- don snydert. Mr. Charles Whittlesey§ designated the different beds of the drift in Ohio and the West as follows : * Geo. Sur. of Canada. + Ibid. t Am. Jour. Sci. and Arts, 2d ser., vol. v. § Lbid. has a os 5. Mesozoic and Cenozoic Geology and Paleontology.. 193 Ist. “Blue hard pan,’ resting unconformably on the surface of the stratified rocks. This is a very compact mass of blue clay, marl and sand, inciuding great numbers of small, partially water-worn, crushed and striated pebbles, principally fragments of: blue limestone and primitive rocks. It contains lime, so much as to effervesce with acids, and to hasten vegetation when applied to land. Beside its strong blue color, it is characterized by imbedded timber, dirt beds, leaves, sticks, and what are called by well diggers “‘ grape vines.’? It is so solid as to be almost impervious to water, and is very difficult to ex- cavate. 2d. “Yellow hard pan,” resting unconformably on the stratified rocks, and the “blue hard pan.” This is a compact material, of a dull yeilow color, with fewer stony fragments or pebbles, and less cal- careous and more aluminous matter than the blue hard pan. It is not quite as solid as the blue, more pervious to water, and contains more and larger pieces of primitive rocks. The clays of the country, used for bricks are principally of this bed. It forms a hard, stiff soil, adapted for grass. The flat regions and savannas of the northwest quarter of the State, are caused by the surface presence of this bed. 3d. “Sand and gravel drift,” containing granite bowlders (in small numbers ), of large size, and unconformable to Nos. 1 and 2, and the other rocks. It exhibits little regularity of stratification, is composed of inferior patches of coarse sand and gravel, intermingled at all in- clinations, evidently the result of long continued and vigorous action of water in rapid motion. The gravel’is coarse, but much worn, rounded and smooth, like the gravel beds of rapid streams. The por- tion of earthy matter is about one half, of a reddish and yellowish col- or, showing the presence of oxide of iron, and containing various pro- portions of sand and clay. Almost every rock in the northern part of America is represented in the gravel; but the greatest part by far is from the underlying and adjacent strata. There are pebbles of quartz, trap, granite, gneiss, conglomerate, limestones of all ages, iron ore, slate, coal and sandstone. In this there has been found timber but very rarely. 4th. The “ valley drift,” eee principally of debris of the ad- jacent rocks, and occupying the lower parts of the great valleys of drain- age. It is more gravelly and less earthy, and the gravel is more of local origin than in No. 3, while the beds of sand are less common. It is in the “ valley drift” or swamp mud that the bones of the mastodon and other large animals are usually found. 194 Cincinnati Society of Natural History. Oth. “ Lacustrine deposits,’ occupying the basin of the lakes, and for Lake Erie, divided into the “ blue marly sand,” and the coarse sand and gravel. The.“blue marly sand,’ commonly called the blue clay of Lake Erie, is seen skirting the shore almost everywhere, if the coast is not rocky,—its upper face nearly horizontal, and rising from forty-five to sixty feet above the water. It is of a light blue color, so fine as scarcely to show between the fingers any grit, homogeneous, and in a dry state compact, but brittle. Very rarely, may be seen a primitive pebble, thin layers of leaves and lignite. It is distinctly and horizon- tally laminated, and at Cleveland is composed of about 75 per cent. im- palpable sand, 3 per cent. iron, 6 to 7 per cent. carbonate of lime, 9 per cent. carbonate of magnesia, and of vegetable matter and sulphur. It is impervious to water, and thus causes thousands of springs to ap- pear at its surface, which, passing out over the edges, dissolve and carry it away very fast, forming a quick sand. Its edge is presented to the action of the waves, which dissolve and carry it away rapidly. As it is not tenacious like clay, and not capable of sustaining itself under its own weight, and that of the sand stratum that rests upon it, there are continual breaks and slides along the banks, on both the American and Canadian shores. These avatanches of earth are from one to four rods in width, breaking off in irregular patches, and some- times sinking, in a night or in a few hours, twenty or thirty feet, leav- ing huge fissures through which the water of the springs passes, and rapidly washes the earth into the lake. At the water’s edge, the slide frequently raises a bank of about the width of the break, several feet above the surface, driving back for a short time the line of the shore. But the waves acting incessantly dissolve the new barrier, and soon commence their attacks upon the body of the fallen mass, which disappears, and is before long followed by a fresh avalanche from above. At the city of Cleveland, where the bluff shore rises 70 feet above the lake, the encroachment since the survey of the town in 1796, has been at the foot of Ontario street, 265 feet. ‘The Canadian shore, from Detroit river to Long point, is losing faster than the American. Be- tween Port Stanley and Port Burwell, on the British side, the superior face of the blue marl is about sixty feet, or fifteen feet higher than at Cleveland, and has in the upper part a lighter or more yellow color. In composition the yellowish portion is more argillaceous than the bright blue, and appears to correspond with the yellow clay stratum of Lake Champlain. The greatest thickness ofthe blue marls can not be com- Mesozoic and Cenozoic Geology and Paleontology. 195 puted, as a large part of it lies below the lake level, forming the bed of more than one half of Lake Erie. On the south shore it extends but a short distance into the interior, forming a narrow belt of low country along the lake, and thinning out as the rocks upon which it rests rise to the southward. The “ coarse sand and gravel” of this division, rests conformably on the “blue marly sand,” and spreads horizontally over a tract of low, and in general wet land, embracing the western half of Lake Erie, and extending westward into the States of Ohio and Michigan. On the north, it forms the soil and surface over a large portion of the peninsula, between Lakes Erie and Huron; which seldom rise more than 200 feet above the waters of these lakes. On it, and composed of its coarse water-washed sand and gravel, are seen the “lake ridges,’ objects of curiosity, and of much utility in a new country, being nat- ural turnpikes that run parallel with the shore. At Cleveland the section is as follows: Ist. Gray, water-washed, coarse sand, resting on the blue marl, 10 feet. 2d. Coarse gravel of the adjacent rocks and sand, 20 to 40 feet. The lake ridges are not precisely horizontal, and are found at various elevations, 30, 90, 120 and 140 feet above the water. There are branches and cross ridges uniting different parallels, that rise and fall several feet in a mile. 6th. Bowlders or “ erratic rocks” which he regarded as a “ stratum,”’ and the newest of all beds except the alluvium. The Drift deposits* are verv extensive on the southern shore of Lake Superior, and more especially on its southeastern coast. There they not only constitute the only visible formations for nearly 100 miles, but they also attain an astonishing thickness, so as to form, by themselves, ridges and cliffs which exceed in height even those of the Pictured Rocks, being in some places, as at the Grand Sable, not less than 360 feet high. The Drift is less conspicuous along the western portion of the lake shore, although it is not wanting even among the romantic and precipitous cliffs of the Pictured Rocks and the Red Castles. The Drift of lake Superior may be divided in ascending order, into— Ist. Coarse drift. This is the least conspicuous of all. It is found only in a few places along the southern shore, generally capping the high towering cliffs of sandstone. It is generally a mixture of loam and fragments of rock of different sizes—sometimes worn, but more generally angular. As a leading feature, it is almost exclusively com- * Foster and Whitney’s Sur. Lake Sup. Region, 1850. 196 Cincinnati Society of Natural History. posed of fragments of the rocks in situ, showing that, whatever may have been its origin, it could not have been acted upon by long con- tinued agencies. A few foreign pebbles exist in it, generally trap, and evidently derived from the neighborhood. Greatest thickness 30 feet. 2d. Drift clay, or red clay. It is a mixture of loam and clay, and. its color is owing to the decomposition of the red sandstone and trap from which it has been derived. It is mainly composed of very finely comminuted substances, yet there are pebbles interpersed through it,and even bowlders of considerable size, generally rounded and smoothed. Fragments of metallic ores and native copper occur occasionally in it— the latter sometimes weighing several hundred pounds. It is found along the whole southern coast of lake Superior, resting upon the red sandstone, and limited to a certain height, but on the Ontonagon and Carp rivers, it is found in depressions on elevated lands, 500 feet above the lake. At Grand Sable where its base rests on almost horizontal strata of red sandstone, a few feet above the water, and its top is covered by a mass of drift sand, it is 60 feet in thickness, and ex- hibits lines of stratification disposed with great regularity. 3d. Drift sand and gravel. This is the most widely diffused of the drift deposits on the shores of lake Superior and the northern part of Michigan. The greatest thickness observed is at Grand Sable, where it is 300 feet thick. 4th. Bowlders. These occur of every size and description in great numbers along the whole southern shore. The largest noticed being of hornblende, and measuring 15 feet in length, 11 in width, and 64 in height. The bowlders have been moved from north to south, but have not come from far, though some of them have been transported from the north shore. It is noticed among the ridges north of Carp river, that the valleys, for the most part, contain bowlders from the next ridge to the north; and there are instances where a ridge did not allow the fragments of the preceding ridge to pass. This limitation pre- vails only within the hilly portion of the Lake Superior region between the lake shore and the dividing ridge. South of thisridge no barrier occurs. 5th. Drift terraces and ridges. These may be seen both on the north and the south sides of Lake Superior, but they are less striking than around Lakes Erie and Ontario. They are most conspicuous on the south shore, between Saut and Keweenaw point. Their average height is about 100 feet. At a place two miles east of Two-hearted river, the following succession occurs: gravel beach, 5 feet ; sand Mesozoic and Cenozoic Geology and Paleontology. 197 beach, 12 feet ; Ist drift terrace, 29 feet; 2d drift terrace, 46 feet ; 3d drift terrace, 75 feet ; summit of plateau, 94 feet. The rocks in many places are grooved, scratched and _ polished. These phenomena, of course, can be seen only where the drift deposits are absent. The groovings consist generally of parallel furrows, from one to four lines wide—sometimes extending a foot, at others many yards. Where the rock is very hard, they are mere striz. Hollow “spots occur, as if they had been scooped out by a round instrument and also wide bowl-shaped depressions, known as troughs, which have been caused by the same agency. Grooves and scratches were ob- served on the road from Eagle river to the Cliff mines running N. 15° E. On an island east of Dead river there are two systems of strize— one running N. and S8., and the other N. 20° E. and 8. 20° W. The rock here which is very hard and tough hornblende, is not only grooved and furrowed over its whole extent, but there are, beside, deep trough- like depressions, with perfectly smoothed walls, some 12 to 15 feet long, 4 feet wide, and 24 feet deep. On Middle Island, east of Granite point, troughs may also be seen 4 feet wide, and 2 feet deep, running like the strie N. 20° E. On the promontories and islands near Wor- cester, two miles west of the mouth of Carp river, there are two distinct sets of strise ; those running N. 55° E. are the most numerous ; thuse running N. 5° E. the least. The latter cross the former and are there- fore more recent. Some of them are, beside, distinctly curved, as if the body which produced them had been deflected in ascending the slope. Each set of striz extends only about one foot below the water’s edge. On the first quartz ridge, one mile from the mouth of Carp river 500 feet high, the strie run N. 20° E. On the iron ridge south of Teal lake, 750 feet high, the strizs run N. 55° E, At the Jackson forge N. 65° E. A green magnesian rock, with vertical walls, and semi- cylindrical form, on the road leading from Jackson landing to Teal lake is covered with strize which may be traced along the surface, like hoops around a gigantic cask. On Isle Royal the strie run N. 50° E. with many local deviations. On the shores of Ackley bay strize near the water’s edge running E. and W., cross others running N. E. and S. W., and others again running 8, 75° E. Isle Royale presents but little evidence of drift, though scattered bowlders are found upon it; the surface of the rock s are generally, however, smoothed, as if polished off. Mr. E. Desor described the superficial deposits on the northern shore of Lake Michigan, the western shore of Green bay, the Big Bay » i! bt pM He ie 198 Cincinnati Society of Natural History. des Noquets, and the valleys of the Menomonee and Manistee. The coarse drift described as occurring beneath the drift proper, at several points along the shore of Lake Superior, seems to be entirely wanting in this district. Starting from Mackinac westward, the furrows and striz were noticed at the bottom of St. Martins bay, and two miles north of Pine river, on a point composed of almost horizontal ledges of limestone, having an average direction from E. to W., some running N. 80° E,, and others 8. 70° and 80° E. At Payment point the direction being from N. 50° to N. 60° E, At the bottom of Big Bay des Noquets, on the west shore of the eastern cove, the direction is EK. and W. At the ~ mouth of the Escanaba, in Little Bay des Noauets, the direction is N. E.and 8. W. At Oak Orchard, on the west shore of Green bay, the direction is N. 15° to N. 20° E. At the saw mill, near the mouth of the Menomonee, the direction is EK. and W.; six miles above Kitson’s trading house, E. N. E. and W.S. W.; three miles above Sturgeon’s falls, N. 65° E.; foot of the Lower Bukuenesec falls, N. 70° E.; Lower Twin falls, N. 60° to N. 70° E.; and at Upper Twin falls, N. 65° to 70° EK. From Green bay, southwestward, they were noticed at Mehoggan point, N. E. by E. and N. N. E.; at Mehoggan falls, N. E. by N.; three miles west of Milwaukee, N. E.; and at Strong’s landing on Fox river, N. E. by E. The true drift seldom approaches the shores of Lake Michigan and Green bay, but it is met with in ascending the rivers at no great dis- tance. Its absence from the coast is the result of subsequent denuda- tion, when the waters of the lake stood at a higher level than at present. It was observed at Pointe aux Chenes, and for a distance of six miles toward Payment point, and on Potawatomee and some of the higher islands. The thickness at Green bay was found on boring to be 108 feet. Near the junction of the Machigamig and Brule, where the united streams take the name of Menomonee, the river banks are composed of drift, forming bluffs 100 feet or more in height. The drift is com- posed of sand and layers of gravel more or less interspersed through it, and covered more or less with bowlders. The higher lands adjoining are covered with the same materials. The country adjacent to the Manistee is likewise covered with the drift sand and pebbles. The whole country drained by the White-fish and its branches, and the Escanaba is likewise covered with the drift. The drift clay is well marked, in many places, below the drift sand, especially upon the é Mesozoic and Cenozoic Geology and Paleontology. 199 Manistee, where it does not generally reach more than 4 or 5 feet above the river, although in one place it was found 10 feet thick. It is very tough, and generally flesh colored, but in one instance it was perfectly white. There were observed, in several localities, rather coarse pebbles of limestone, and even flat stones intermixed with the upper layer of | clay, near its contact with the sand. He described the terraces on the island of Mackinac and the neigh- boring coasts, on the west coast, and at Pointe St. Ignace and Gros Cap on the north coast of Lake Michigan, which vary in height from 20 to 130 feet. But the terraces are not found farther west on the north shore of Lake Michigan and Green bay, nor in the vicinity of the Menomonee and Manistee. Mr. Charles Whittlesey,* said of the terraces bordering Lake Erie, that the first ridge, or that nearest the lake, is known as the “ North ridge.” From Conneaut, in Ashtabula county, to Russelton, Huron county, a distance of 120 miles, the elevation of the ridge above the lake varies from 85 to 145 feet. The second ridge, from Kingsville, in Ashtabula county, to Ridgeville, in Lorain county, varies from 122 to 168 feet above the lake. These ridges consist of coarse, water-washed, yellowish sand, or of fine gravel, principally the comminuted portions of the adjacent rocks. The rocky fragments are not generally worn per- fectly round, or oblong, as beach shingle is, but are more flat, with worn edges. There are mingled with the sandstones and shales that compose this gravel, scattered pieces of quartz, flint, granite, trappean “rocks, limestone and ironstone. The third and fourth ridges are a little higher, and composed of coarser material. In 1852, Charles Whittlesey+ described the drift in that part of Wis- consin bordering on Lake Superior, and lying between the Michigan boundary and the Brule river, and the sources of the streams flowing into Lake Superior from the south. He divided the drift into—Ist, red marly clay; 2d, bowlder drift, coarse sand and gravel. The red marly clay is a fine-grained, homogeneous marly sand, cemented by argil or clay, with well defined horizontal lines of lamina- tion or deposition; containing, but very rarely, pebbles of granitoid, trappose, sandstone, conglomerate, or slate rocks. This constitutes the shore or lake bluffs most part of the way from the Montreal to the Brule; the red sandstone, on which it rests, showing itself occasionally beneath. It is easily washed away in suspension by the waves, and * Am. Jour. Sci. and Arts, 2d ser., vol. x. t Owen’s Geo. Sur., Wis., Iowa, and Minn. 200 Cincinnati Society of Natural History. having little tenacity, falls in slides and avalanches into the water, and is thus cut into deep, narrow gallies by rains. Its surface in the above district is not more than 250 feet above the lake, sloping gradually from the mountains to the shore, as though it formed, at one time, the bed of an ancient sea. On the waters of the St. Louis river on the west, and the Ontonagon on the east, however, the red clay deposits reach to the height of 450 to 500 feet above the lake. On the “ Isle aux Barques” the lime is so abundant in the clay, that it has formed in amorphous concretions throughout the mass. A few leaves and decayed sticks have been seen in the red marly clays, with carbonaceous matter and lignite, but such occurrences are rare. Along the coast there are interstratified beds of sand and gravel of a local character. In the interior, where the clay is visible in bold bluffs, along the water courses, it is more uniform and less inter- calated with coarse drift. It rests not only on the sedimentary unaltered rocks, but also on trap and metamorphic and igneous rocks. The mass of the hills between Chegwomigon bay and the Brule river, is gravel and bowlder drift. It is not very uniform in composition, and is marked by the violent action of water. The central part of this peninsula presents large tracts of barren, water-washed land, and mod- erately coarse gravel. Both the western and eastern knobs and ridges are of coarse materials; and toward the point or extremity about the “detour,” and the adjacent islands, the sand and bowlder deposits are represented. A section of three miles from the coast to the mountains, four miles southwest of La Pointe, showed red marly clay 95 to 130 feet above the lake, capped by coarse bowlder drift, the top of which is 428 to 509 feet above the lake. This drift is disposed in three very abrupt and well defined terraces. These terraces continue southward around the southern extremity of the mountain, and have the appearance of ancient beaches or shores. In 1855, Prof. G. C. Swallow* found a fine, pulverulent, absolutely stratified mass of light, grayish buff, silicious and slightly indurated marl, capping nearly all the bluffs of the Missouri and Mississippi within that State, for which he proposed the name Bluff formation. The Bluff above St. Joseph exhibits an exposure 140 feet thick. It is easily penetrated by the roots of trees, which decay and leave en- crusting tubes, giving it a peculiar perfurated appearance. It extends from Council Bluffs to St. Louis, and below to the mouth of the Ohio. * Geo. Sur. of Missouri. Mesozoic aad Cenozoic Geology and Paleontology. 201 The greatest development is in the counties on the Missouri, from the Iowa line to Boonville. In some places it is 200 feet thick. At Boon- 3 ville it is 100 feet thick, and at St. Louis only 50 feet. The Bluff Group is older than the bottom prairie, and newer E than the Drift. It gives character and beauty to nearly all the best landscapes of the Lower Missouri. He found the drift abounding north of the Missouri river, and ex- isting in small quantities as far south as the Osage and Meramec. Its thickness varies from 1 to 45 feet. The upper part, having the ap- pearance of having been removed and rearranged by aqueous agencies since its first deposit, but before the deposit of the Bluff Group, is described as altered drift. The heterogeneous strata of sand, gravel, and bowlders, is called the bowlder formation; and below this, in some places, « third division exists, which is called the “pipe clay.” It contains bowlders more or less dispersed through the upper part of it. It is found in Marion, Boone, Cooper, Moniteau, Howard and Monroe counties, varying in thickness from | to 6 feet. William P. Blake* described the grooving and polishing of hard rocks and minerals by dry sand in the Pass of San Bernardino, Cali- fornia, and on the projecting spurs of San Gorgonia, he said, grains of sand were pouring over the rocks in countless myriads, under the in- fluence of the powerful current of air which seems to sweep constantly through this Pass from the ocean to the interior. Wherever he turned his eyes—on the horizontal tables of rock, or on the vertical faces turned to the wind—the effects of the sand were visible; there was not a point untouched, the grains had engraved their track on every stone. Even quartz was cut away and polished; garnets and tourmaline were also cut and left with polished surfaces. Masses of limestone looked as if they had been partly dissolved, and resembled specimens of rock salt that have been allowed to deliquesce in moist air. These minerals ; were unequally abraded, and in tbe order of their hardness; the wear ¥ upon the feldspar of the granite being the most rapid, and the garnets being affected least, wherever a garnet or a lump of quartz was im- bedded in compact feldspa:, and favorably presented to the action of the sand, the feldspar was cut away around the hard mineral, which was thus left standing in relief above the general surface. A portion however, of the feldspar, on the lee side of the garnets, being protected from the action of the sand by the superior hardness of the gem, also stood out in relief, forming an elevated string, osar like, under their DD? * Am. Jour. Sci. and Arts, 2d ser., vol. xx. 202 Cincinnati Society of Natural History. lee. When the surface acted on, was vertical and charged with gar- nets, a very peculiar result was produced; the garnets were left stand- ing in relief, mounted on the end of a long pedicle of feldspar, which had been protected from action while the surrounding parts were cut away. These little needles of feldspar tipped with garnets, stood out from the body of the rock in horizontal lines, pointing like jeweled fingers in the direction of the prevailing wind. The effects of driven sand are not confined to the pass; they may be seen on all parts of the desert where there are any hard rocks or minerals to be acted upon. On the upper plain, north of the Sand. Hills, where steady and high winds prevail, and the surface is paved with pebbles of various colors, the latter are all polished to such a de- gree that they glisten in the sun’s rays, and seem to be formed by art. The polish is not like that produced by the lapidary, but looks more like laquered ware, or as if the pebbles had been oiled and varnished. On the lower parts of the desert, or wherever there is a specimen of silicified wood, the sand has registered its action. It seems to have been ceaselessly at work, and when no obstacle was encountered on which wear and abrasion could be effected, the grains have acted on each other, and by constantly coming in contact have worn away all - their little asperities and become almost perfect spheres. This form is evident whenever the sand is examined by a microscope. We may regard these results as most interesting examples of the denuding power of loose materials transported by currents in a fluid. If we can have a distinct abrasion and linear grooving of the hardest rocks and minerals, by the mere action of little grains of sand, falling in constant succession, and bounding along on their surface, what may we not expect from the action of pebbles and bowlders of great size and weight, transported by a constant current in the more dense fluid, water? Wemay conclude that long rectilinear furrows of indefinite depth may be made by loose materials, and that it is not essential to their formation that the rocks and gravel, acting as chisels or gravers, should be pressed down by violence, or imbedded in ice, or moved forward en masse under pressure by the action of glaciers or stranded icebergs. Wherever, therefore, we find on the surface of moun- tains, not covered by glaciers, grooved and polished surfaces with the furrows extending in long parallel lines seeming to indicate the ac- tion of a former glacier, we should remember the effects which may be produced during a loug period of time by light and loose materials transported in a current of air; and which, consequently, may be pro- Mesozoic and Cenozoic Geology and Paleontology. 203 duced with greater distinctness, and in a different style, by rocks moved forward in a current of water. The effects produced by glaciers, by drift, or moving sand, are doubtless different and peculiar, so dif- ferent and characteristic, that the cause may be at once assigned by the experienced observer, who can distinguish between them without difficulty. Itis, however, possible that after a sand worn surface, such as has been described, has been for ages covered with moist earth, a decomposition of the surface would take place sufficient to remove the polish from the furrows and leave us in doubt as to their origin. Alexander Murray* examined a portion of the country between Georgian bay in Lake Huron, and the Ottawa river. He followed the course of the Muskoka river to its head, and by a short portage passed to the source of the Petewahweh, and by its channel de- scended to the Ottawa. Returning, he ascended the Bonnechere river to Round lake, from which he crossed to Lake Kamaniskiak on the main branch of the Madawaska, and descended the latter stream to the York or southwest branch, from whence he crossed to Balsam lake. He found stratified clays on the Muskoka, between the lake of Bays and Ox-tongue lake, at the height of about 1,200 feet above the level of the sea; the banks expose 10 or 12 feet in thickness, of drab or light buff-colored clays, alternating with very thin layers of fine yellow or grayish sand, At one place, the beds are tilted, showing a westerly dip of about eight degrees, in which they exhibit slight wrinkles or corrugations. Coarse yellow sand overlies the clay, and spreads far and wide over the more level parts, generally forming the bank of the river, where not occupied by hard rock. On the Petewahweh, especially below Cedar lake, the whole of the level parts are covered with sand, which, in some places, is of great thickness. Cedar lake is about 1,050 feet above the sea. The banks or the Bonnechere display a great accumulation of clay at many parts below the fourth chute, sometimes exposing a vertical thickness of from 70 to 80 feet. Near the mouth of that river, below the first chute, where the clays form the right bank, and are upward of 50 feet high, they are chiefly of a pale bluish-drab color, and are calcareous, while other clays found higher up the stream, are of a yellowish-buff, und do not effervesce with acids. Below the second chute, buff-colored clay is interstratified with beds of sand and gravel, the latter sometimes strongly cemented together by carbonate of lime, the whole being overlaid by a deposit of sand. The gravel is seldom f } et eee ee eee e 1 * Geo. Sur. of Can., Rep. of Progr. for 1853. aliases tiles Ss Cer EN et aad basal Ea ele 9 ca il ik’ apes oa 204 Cincinnati Society of Natural History. very coarse, although an individual bowlder may occur here and there amongst it, and it is chiefly derived from the rocks of the Laurentian series. The height of the first chute above the sea, is 265 feet; the second chute, 348 feet; the fourth chute, including its fall of 39 feet, 432 feet; Round lake, 520 feet, or nearly 60 feet below Lake Huron. Sand is extensively distributed over the plains of the Bonnechere, and over a large portion of the area between it and the valley of the Madawaska. Most of the valley of the Little Madawaska is covered with sand on either side, and the country between its head waters and Lake Kamaniskiak is one continuous sandy plain. The height of land in passing over the portage to the Madawaska is 968 feet abuve the sea, and Lake Kamaniskiak is 906 feet above the level of the sea. No organic remains have been detected in any of these drift deposits. — He, afterward,* surveyed the valley of the Meganatawan river and part of the coast or Lake Nipissing. Stratified clay was found on the banks of the Meganatwan, above the second long rapids, east of Doe lake. The color is a brownish drab; it is very tenacious, and does not effervesce with acids. The highest exposure is a little over 1,000 feet above the level of the sea. A fine, strongly tenacious clay occurs on the Nahmanitigong near the main elbow, where the upward course of the river turns to the south at an elevation of 710 feet above the sea. The color of the clay is chiefly pale drab or buff, but bands of reddish clay are interstratified and some of pale blue overlie the whole. The clays of the interior are usually overlaid by a deposit of coarse yellow sand. Among the bowlders on Lake Nipissing, many were observed to be of a slate conglomerate like that of the Huronian series, and they were frequently of very great size. . In the succeeding year+ he explored portions of the Huron and wes- tern districts of the Province of Canada, and found that the course of — the currents which had borne along the drift was from northwest to— southeast. This is indicated by the pebbles and bowlders of metamor- phic rocks which were clearly derived from the Laurentian and Huron- ian formations on the north shore of Lake Huron, and by the character of the fossiliferous rocks and pebbles which have been moved a shorter distance, and by the grooves and scratches which invariably have a bearing from the northwest to the southeast. He, afterward,{ made a survey north of Lake Huron, where he found SK ee ee * Geo. Sur. of Canada., Rep. of Prog., 1854. + Rep. of Prog. for 1855. t Rep. of Prog. for 1856. . vs Mesozoic and Cenozoic Geology and Paleontology. 205 bowlders derived from the Huronian rocks that had been moved from | their source and transported southerly. In the valleys of the Wahna- _ pitae and French rivers, large bowlders of conglomerate rest on the contorted oneiss at various elevations above the mark of the greatest floods, the highest probably over 100 feet. On the Sturgeon and Mas- kanongi rivers, and on Lake Wahnapitaeping, the course of the grooves and scratches is S. 27° W., with scarcely any deviation, but farther west they seem to alter their course to a more westerly direction, and on Round lake they bear S. 41° W.; while at the long lake, near the outlet of the White-fish river, their direction is $. 49° W. The great deposits of silicious sand, which are spread over the upper valley of the Wahnapitae, above Wahnapitaeping lake, and also the sand in the valley of the Sturgeon river, are probably chiefly derived from the ruins of the Huronian rocks. Lake Huron is 578 feet above the sea; Lake Wahnapitaeping, 938 feet ; Round lake, 775 feet ; Sturgeon river, at the junction of the Maskanongi, 809 feet; and Maskanon- giwagaming lake, on the Maskanongi, 862 feet. In 1859, he described* the drift north of Lake Huron, between the valley of the Thessalon river and the lake coast south of it, and be- tween the valleys of the Thessalon and the Mississagui. ( 1660| 187 eeretii0| 151 g 1 Dal) 3h Z| 1337| 169 Breadth. ITudex of Breadth. Index of Height. © jee (ae: | * 10 sei a 0) |\ *) ee 0, 6 <6 a) ejuel 0! 0/6 see eee ee ew © «ife) (6) ati velue ree ewe sec eee 200 Ase) Width of Frontal, ee eee else 23 93] i | = ° =e Ba iS) &0 ee > N se 135 34 134 oH 124 32 132 36 133 36 131 34 159) 34 140 36 142 36 be Lutes, 36 peers 38 133 33 138 32 139 36 132 3) Asi 34 143 38 119 35 131 33 138 30 138 38 144 37 ee: 39 136 Sal 130 35 131 38 139 oe 157 39 119 ou 38 8 136 35 = fo) S Se E Po 42 ie 40) M. 37 FE. pea ele FE. M. aee M. 41 F. 38 F. 38 F, 43 M. 40) M. Lee Brno 40} . A0 |e ae 40} . 38 M. 44 M. 39) F, 45 M. 47 M. 43 M. 42 1m, 40 M. 43 M. 42 M. ipl F, 41 F, 4] 1D A( F. 43 M. 43 M. 46)Max. 37| Min. 9) Range 40 5|Mean. * These figures refer to the number of crania measured in each particular respect. 240 Cincinnati Society of Natural History. The following notes are based on an examination of the 83 crania given in the above table, and 58 others not yet measured, making 141 in all, this being the entire number sufficiently preserved to be available for measurement, although 662 skeletons, of allages, have been exhumed to date. The peculiarities presented by the crania and other bones will be con- sidered under several heads, as follows : 1. GENERAL ConrtTOUR. SIZE. SPECIAL CHARACTERISTICS OF THE VARIOUS BoNES AND CAVITIES. SUTURAL PECULIARITIES, INCLUDING WoRMIAN BONES. PHYSIOLOGICAL CHARACTERISTICS OF THE Lone BoNEs. . PATHOLOGICAL FEATURES. Ae many of the crania are more or less imperfect, it will be necessary for statistical accuracy to state explicitly under each heading the num- ber of crania examined in that particular connection. The section relating to the crania will be followed by an account of the various physiological and pathological peculiarities observed in gists portions of the skeleton. Sa eet (1.) As regards their GreNERAL Contour, the crania are, generally speaking, of the brachycephalic type, having a cephalic index (index of breadth) of .800 and over. An examination of the 72 given in the table which are available for study in this respect, shows them to be divided as follows : Dolichocephali (index of breadth, .730 and under) ..... 3 Orthocephali i (index of breadth, .740-.00) ..... 2: yee We Hi Brachycephali (index of breadth, .800 and over) ....... 52 Total, 2.208) eae ee 72 In common with most, if not all, North American aboriginal crania, they are also characterized by a markedly pyramidal form as viewed anteriorly, this being due chiefly to their great zygomatic diameter, a feature characteristic of the mongoloid races generally. Flattening of the occiput, also a characteristic of most American aboriginal crania, doubtless due to the custom of strapping infants on a cradle-board, is a rule amongst these to which there are few excep- tions; and where, as is often the case, this flattening has been more or. less unilateral, plag/ocephalism or oblique asymmetry of the general cranial development, has resulted. . : ; a et , aw ye The Madisonville Pre-Historic Cemetery. On the other hand, none of the crania show any traces of the antero- - posterior flattening of the frontal bone, which is said to have been a _ eustom among the Natchez, Chickasaws, Choctaws, and perhaps some other tribes of this region. The absence of this flattening, so far as it goes, tends to exclude the probability of this people being identical with either of the tribes mentioned. Prognathism is a generally well-marked, though not constant feature of these crania. No. 49, in the above table (fig. 1), is remarkable for its great length, both absolute and as compared with its breadth, which latter dimension, however, can not be obtained accurately, as a portion only of the WA SW Fig. 1. Cranium remarkable for its peculiar proportions and prominent supra-ciliary ridges (No. 49 on table). calvarium is preserved. In its peculiar proportions, low, narrow fore- head and prominent supra-ciliary ridges, it bears a somewhat striking resemblance to the famous Neanderthal skull, its length, however, bes ing greater, and the forehead narrower. x > [: Freee \ eee 242 Cincinnati Society of Natural History. (2.) With respect to Sizp, numbers 4, 5 and 12 on the table are noticeable as representing the two extremes ; No. 4 being the sixth in point of size of all aboriginal American crania on record,* The following table of comparative measurements will explain better than words the average proportions of these crania, as compared with those from other localities in North America. Comparative Table of Cranial Measurements. =) eee = se = 2 E S e Sl oe aie S) = ne} a Pa S - | 2 | 8 | 3 | ee O 4 en aa as a =< Mean of 83 erania from| 4st 78t T7t 61t 72 58t 69t Madisonville. Bats. 1337 109 139 135 .825 799} 93 Mean of 67 crania from 30 67 6k 40 stone-graves in Tenn.| 1341 166 | 141 142 .852| .804) 91 Mean of 21 crania from 18 21 21 21 stone-graves in Tenn.| 1335 165 143 141 O72) Sonera Mean of 38 crania from 24 37 38 36 a mound in Kentucky.| 1313.33} 165.4) 142.28) 182 857, .769) 92.7 Mean of 10 erania from 2 10 8 4 caves in Ky. and Tenn.| 1382 168 | 140 143 831} .823) 90 Mean of erania from 39 118 115 78 mounds in U.S .....° 1374 168 145 139 867; .821 Mean of 18 crania from a 16 18 Tut Mlorida.. 024). See 1375 7 173.5| 145 185.6] .830| = .777| 98.47 Mean of 103 crania from Santa Barbara, Cal....| 1248 L7bag tsb 129 779| = .741) 98 Mean of 50 ecrania from Islands off Santa Bar- bara; California...;... 1326 184. 133 128 .(23| 680) 93 Wew Englands. ta..s) o/s. 2. «)) AR ores 136 OO) >, dae ae MET AUOUS ais, cere). patsascage | owe, ee Bie oi tel es 15 7/ 137 TAO; TAO ee stat AT OOINOMUM et ota g eis [2 ae on .| 184 141 136 .f OO) are Algonquin (Lenape) ..| .......{ 180 | 140 137 epee fly os ae Ee sauiiniaixn) eo Ae Pee ces salt el ee ley 138 TOA Toe PSCHUKEC Tes, coe Bee: Sail apd. 135 137 OT ise The capacity of the average European skull is given by different authorities at 1510 to 1531 «. c. The index of breadth ranges from .750 to .800 in the various European nations, being lowest (.750-.760) * This skull has been described and figured in a previous paper; see this JOURNAL, vol. iii., p. 54, plates 2 and 3, t+ This table, with the exception of the first item, is taken from the Eleventh Annual Report of the Peabody Museum of American Archeology and Ethnology, 1878, p. 368. { Tue small figures refer to the number of crania measured in each particular respect. Lo The Madisonville Pre-Historic Cemetery. 243 in the Anglo-Saxons, ancient Romans, and Roman British, and highest in the English (.770), French (.780), German (.790), and Prussian (.800 ).* (3.) SpectAL CHARACTERISTICS OF THE VARIoUS BoNES AND CAVITIES oF THE HEap. The Temporal Process of the Malar Bone. The writer takes the liberty of reproducing here his descriptiont+ of this process, with some additional data respecting the frequency of its occurrence. “ A noteworthy anatomical and possibly anthropological feature of a large proportion of the crania from the well known ancient cemetery near Madisonville, Ohio, is the presence of a spine-like and occasion- ally unciform process, situated on the-posterior border of the malar bone and partially covering in the temporal fossa. This projection, for which the writer proposes the name ‘temporal process,’ is some- what triangular in shape, its base, which is from 7 to 18 mm. in length, being continuous with the middle third of the posterior border of the bone; it tapers somewhat rapidly to its rather obtuse apex, its length varying from 4 to 8 mm. “It is of occasional occurrence also in negroes and mulattoes, and further observations as to its distribution and frequency in various races would doubtless be of interest.” Fig. 2 illustrates a well developed example, as seen in many of the Madisonville crania. Of 68 crania from the Madisonville cemetery, observed with reference to this process, it is present to the following extent: Well developed (attaining a length of 83 mm. and over)... 52 Euaimentany(lessrthan 3 mm-)\ 6... 12.20. e lo. 13 LE TOSEIING.. oo a SG ad che ae NED SREE AE a legn EE eee ee 3 mI OUaul PRE ere ere asec ly ls Ct 68 In one case it is observed to attain a length of 8 mm., and a width at base of 19 mm. Since the above announcement of this process, it has been observed in the two Australian crania in the museum of this Society; and in the cranium of a Buginese in the Mussey collection at the Miami Medi- * Vide “Thesaurus Craniorum,” by Dr. Barnard Davis, pp. 352-359, 7 Read before the American Association for the Advancement of Science at its thirtieth meeting. Ciucinnati, August, 1881. ee. ee TA es 244 Cincinnati Society of Natural History. cal College; of three Bengalese crania in the latter collection it is well marked in one, rudimentary in another, and absent in the third. PEE ZL A fi é a = ! ==ZAF-e FF EEE OPO Zagz BBB BZ FZ Fig. 2. Lllustrating the temporal process of the malar bone. In 138 modern crania, from various sources,* examined with refer- ence to this feature, it is present as follows: * Museums of the Miami and Ohio Medical Colleges, and of the Cincinnati Hospital. The Madisonville Pre-Historic Cemetery. 245 Well developed (3 mm. and over in length).......... 6.48 Eacimentary (less than 3mm.).................5...4: 33 PN He ee ee be ee ell 57 TOBE cs saben a ap eee 138 The nationalities of these crania can not be ascertained, but it is reasonable to assume that a considerable proportion of them are from negroes and mulattoes. This process is probably a more or less constant feature in American aboriginal crania generally, and it seems somewhat remarkable that so acute an observer as Morton should have overlooked it in his ex- tensive craniological investigations; such, however, appears to have been the case, as no mention is made of it in his elaborate work, entitled ‘“Crania Americana,” although well-marked examples are figured in Plates 116 (Peruvian), 12 (Orinoco Indian ), 15 ( Botocudo), 17 and 18 (Mexican ), 19, 20, 23, 25, 28, 30, 31, 37, 39, 41 and 47 (the last eleven all North American Indian), Peculiarities of the Cavities. The orbits are, to the eye, noticeable for their marked angularity, and for their great width as compared witb their height, but as no series of measurements of these cavities in other races is at hand, it is impossible to institute a comparative study of this feature at present. As regards the nasal cavities these do not present, to the eye, any noticeable variation in size as compared with those of Caucasian skulls, but no details of measurement have yet been made on this point. The external auditory meatus in these crania is generally elliptical in form, its long diameter extending vertically or nearly so. Bony out- growths or tumors are observable near the outer opening of this canal in five of the 83 crania examined. In three of these instances the ex- ostoses are limited to one side; in the other two they occur in both ears. In one skull the meatus is so obstructed by these growths that its lumen is quite obliterated on one side, and nearly so on the other. With respect to the other openings of the skull, mention may be made here of a quite general narrowing of the spheno-mazillary fissure, due to approximation of the orbital process of the superior maxilla and the orbital surface of the great wing of the sphenoid ; these sur- faces even articulating slightly in some instances as noted further on under head of sutural peculiarities. (4.) SururAL PECULIARITIES, INCLUDING WorRMIAN Bones. Persistent Frontal Suture. , In one skull, not yet measured, and consequently not included in the 246 Cincinnati Society of Natural History. above table, the frontal suture is persistent throughout, being the only instance of its occurrence noted in an examination of 141 adult crania from this cemetery. In this connection, the following table relative to the frequen of persistent frontal suture in various races is of interest; it is taken from Peschel, “ Races of Man,’’ N.Y., 1876. SKULLS Proportion of ISSR EWS With Without ae es An Open Frontal Suture. Skulls. Germans oteballen dee Bier ea chile ccd: 70 497 dicey it Inhabitants of St. Petersburg.... .. 70 1023 1:14.6 Other Caucasians *..' 258 we). es. OS. 14 129 1292 IEGMO OI vhs ee eh Cree ot). te: Het 7 96 1213.7 JU Ee) I A AP eet: eked ae a ee ee ates 5 87 171i INGeTroes! ese ait ts: ER eae em baie 1 52 1 352 Americans) Mintek meat ivan de by. il 53 1:53 The skull from Madisonville in which this suture is persistent, ap- pears to be that of an individual of from 45 to 50 years of age, and presents various other abnormities, as follows: A so-called “inca” (wormian) bone, situated at the apex of the lambdoid suture; an- other wormian bone at each end of this suture, and several smaller ones scattered throughout its continuity ; six small wormian bones in the left squamo-parietal suture, and one in the same suture on the right side; on the right side one, and on the left two, su- pernumary bones intervene between the tip of the great wing of the sphenoid and the anterior inferior angle of the parietal. The incisive suture is partially persistent in 18 out of 62 crania ex- amined in that connection. The so-called “inca bone,” which is merely a triangular wormian bone replacing the apex of the occipital, is present in 14 of the 88 crania examined in this respect. In two of these it attains a very large size, replacing almost the entire upper half of the occipital. This is the case in No. 79, where the “inca bone’? measures 88 mm at the base, and 46 mm, from centre of base to apex, the outline of its lower border being somewhat crescentic. An additional wormian bone, of small size, is placed between it and the parietal on the left of the median line. {n the same 88 crania other wormian bones are fre- quent, being distributed amongst the various sutures, as follows: In the lamdoidal suture in 26 instances, the number of bones in each case varying from one to four or five ; in the occipito-temporal, 5 in- stances ; squamo-parietal 1; fronto-parietal, 1; spheno-parietal, 4; spheno-temporal, 1; spheno-malar, 1. The Madisonville Pre-Historic Cemetery. 247 Synostosis, more or less complete, of various sutures, is observed in 13 crania out of 68 examined ; the following being the lst of sutures affected : RO bey) 3 es a gio awe en Re) Ere demTl@nClall eo. ak) e peovee edi OOS © Cho eee See aa an 1 UEDA! » 5 a Meals ieee racic otis oleae ene nn Pa 8 iC [DEVO OORT CHE Ghewielsecs cys a sl 5 ea ae 1 ‘iD AMEIROSIMOLN EST Bye tole ER a hake a itch, eae nek Av ana I i a aaa ede 4 DCMU C MIMASCOUL nan cIeren rie ieee yey LISS be sleds 1 IMI OTT OU Ae Toor anal ar UA ot BS i Aare wa our a 1 Articulation of the Superior Maxilla with the Sphenoid. Of 55 crania examined with respect to this feature, the orbital pro- cess of the superior maxilla articulates directly with the orbital sur- face of the sphenoid, as follows: On one side only, in three instances ; on both sides, in four instances. (5.) PHystoLoGicAL CHARACTERISTICS OF THE LonG Bongs. Perforation of the olecranon fossa. Of 34 humeri examined with reference to perforation of the olecran- on fossa, this condition was found to be present in 17; it is possible, however, that some of these were selected for preservation on account of this feature, so that any final conclusions drawn from these figures might be fallacious. Wyman,* in an examination of 80 Indian humeri in the Peabody Museum, found 25 perforated (about 31 per cent.); of 52 humeri of whites, this condition was present in only two. It is a quite general characteristic of the Anthropoid Apes. Plactycneism, or lateral flattening of the tibia, is a well-marked characteristic, but for lack of comparative measurements no definite details can now be given respecting this feature. Cnemeolordosis, or antero-posterior curvature of the tibia, appears to be tolerably constant, but does not attain a high degree of develop- ment except in the diseased tibiee. (6.) PaTHoLocicaL FEATURES. The following notes embrace all cases of disease and injury of the bones observed to date. 662 skeletons have been exhumed, each of which has been carefully examined for marks of disease or injury, and it is believed that few, if any, cases have been overlooked. * Fourth Annual Report of the Peabody Museum of American Archeology and Eth- nology p. 20, Boston, 1871. 248 Cincinnati Society of Natural History. Pathological conditions of the crania. Ankylosis, complete, of the condyles to the articular surfaces of the atlas, is present in three crania out of the 141 examined. One of these ee ee ee eee ere eee Fig. 3. Ankylosis of vertebral column. 38a, Axis and third cervical vertebre. belonged to the unfortunate possessor of the spinal column and other bones referred to in a previons paper,* as follows: * This JOURNAL, VOl. iii., p. 139. The Madisonville Pre-Historic Cemetery. 249 “The spine of this individual (see fig. 3) presents an example of a somewhat remarkable pathological condition, the spinous and articular processes of all the dorsal and lumbar vertebree being ankylosed; the bodies remain free, with the exception of two in the lumbar region, which are connected only by a thin band of osseous tissue. The last lumbar vertebra is in its turn solidly united with the sacrum, and the latter bone with the ilia. Several of the carpal and metacarpal bones are also united into a solid bony mass, and the atlas is connected with the skull in a similar manner, altogether making this one of the most interesting cases of disease of the osseous system on record.” In ad- dition to the above-named conditions mention should have been made of the fact that the axis and third cervical vertebre are also united by coalescence of their bodies as well as of their transverse, ar- ticular and spinous processes. The heads of all the ribs are likewise ankylosed with the bodies of the vertebree, and their tubrosities with the transverse processes. While the antero-posterior curvature of the spine is marked, it will be observed that this has not been due, as in Pott’s Disease, to a breaking down of the vertebral bodies. The general implication of the articular surfaces can leave no doubt as to the constitutional nature of the disease, which was probably that now recognized as Chronic Osteo-arthritis, or according to some authors, arthritis deformans. In the above-mentioned skull and one other, evidences of arthritis are present in the temporo-mazillary articulation, on the right side; in both cases obliteration of the glenoid fossa has resulted from new bony deposit. In a second specimen of ankylosis of the occipito-atloid articulation, bony union has likewise occurred between the transverse processes of the atlas and the jugular processes of the occipital. Two or three of the crania exhibit a carious appearance of the vault of the skull, but whether this is due to inflammatory processes or not, is difficult to determine on account of their advanced state of decay. Fractures of the Skull and Facial Bones. Of the 141 crania examined, eleven exhibit evidences of fracture, as follows : Fracture of the right parietal, extending from the anterior inferior angle upward and backward for 65 mm. through that bone ; a deposit of new bony matter along its edges indicates some attempt at repair, which, however, has never been completed. One specimen shows an indentation of the outer table over the right frontal eminence. 250 Cincinnati Society of Nataral History. There are two cases of marked indentation of both tables in the poste- rior parietal region, both evidently the result of blows from a blunt instrument ; one of these is shown in fig. 4. A marked indentation near the apex of the vertical plate of the frontal bone, probably from same cause as the preceding. tii ee, { 1 \\ rt \ H, ai i } ji My —\ . \\ \\\ NAN Mi (WA) i wit 22. BAW 2 e) a / Wi ff | HT wm / f ly Fig. 4. Depressed fracture of both tables, followed by repair. Two specimens exhibit perforation of the left parietal, near its posterior border, with marked depression of the inner table ; in both of them recovery has apparently ensued, as the openings are partially af. | — Lad of Fig. 5. Perforating fracture of the left parietal near its posterior superior angle; internal view, showing the depressed fragment of the inner table, which has re-united. (Natural size). closed by new bony deposit, and the remaining edges nicely rounded off. One of these, showing the depressed fragment of the inner table, is represented in fig. 5; the other in figs. 6 and 6a. Find eitie as eae. 0 yr oe, ws : ON, em “De The Madisonville Pre-Historic Cemetery. | 251 Figure 7 illustrates the results of an extensive injury to the frontal and right parietal bones, followed by prolonged suppuration and for- Sz aA =} SS i Y LE a im ti! SSS AAD vo BZ g SIs ) ON SA UAL et Za { AL LIN CE Nh eae ae FV 4 > hy Se

a r 255 “‘SOUO SUOT OY} JO SUOISO[ SHOLIVA JY} JO SUOTIVAYSNITT SWYV/TTIN lle Pre-Historic Cemetery. —aNa— ‘a°NI9 tSONUE The Mad 0 “SLA ‘61 “SIA “8ST SI "1 SLA 2 ee ee i 256 Cincinnati Society of Natural History. the surgical neck of the humerus; and figure 13 the result, probably, ot a “green stick” fracture of the same bone in its middle third. The adage that nature is a better physician than surgeon is illus- trated by a case of fracture of the femur above the condyles (fig. 21). The figure shows the posterior aspect of the bone, and it will be ob- served that in this instance the lower fragment is displaced forward, and the upper backward, contrary to the usual result in such fractures. Another femur presents an enlargement on its posterior surface at the lower bifurcation of the linea aspera, which appears on section to be due to a simple hypertrophy of the compact tissue: the same speci- men shows asmall, circumscribed, roughened exostosis on the articular surface of the inner condyle near its posterior border, The pathological features presented by the tibize, include evidences of periostitis, osteitis and osteo-myelitis, in varied combination; as well as exostosis, and an obscure form of rarefaction. Figure 14 illustrates enlargement and distortion of the tibize follow- ing periosteal inflammation ; the evidences of ulceration about the lower half of this bone are somewhat suggestive of syphilitic lesions, which supposition is further strengthened by the bilateral character of the disease, and the presence of several nodular excrescences dis- tributed along the crest of the bone. Figure 15 also illustrates bi-lateral disease with enlargement and distortion of the general contour of the bone, probably the result of osteitis; in this case a cross section shows almost complete obliter- ation of the medullary cavity by extensive deposit of cancellous bone, as well as considerable increase in the density and thickness of the compact tissue,—conditions characterized by the term osteo-sclerosis. Figure L6 represents one tibia of a skeleton exhumed during the ex- cursion of the American Association for the Advancement of Science, on August 22, 1881. It is remarkable for the extreme rarefaction of the bone, the compact tissue being reduced to a mere shell, and the medullary cavity almost filled with an abundant deposit of spongy cancellous tissue. Its fracture was post-mortem, due to carelessness of a member of the audience. The disease is bi-lateral, limited to the tibiw, and resembles what is known as rarefying osteitis. The subject was a very old person. Unilateral disease of the tibia resulting in hyperostosis, is shown in figure 17. Osteitis, involving the tibia, and fibula, and resulting in an extensively diffused new bony deposit is illustrated by figs. 18 and 19. Both tibiz — and fibule were similarly affected. The Madisonville Pre-Historic Cemetery. 207 Exostosis of Tibia. A circumscribed spongy or fungous exostosis of the tibia is shown in figure 20. It is limited to the upper half of the bone, and to its posterior and external surfaces, the underlying compact wall being in- volved in the diseased process to some extent. The same specimen shows a hemispherical cavity with smooth walls and edges, large enough to admit a filbert, in the head of the bone just above its tuber- osity. Correction.—Later advices from the Peabody Museum, necessitate changes in the capacities of two of the Madisonville crania sent to that institution; the effect of these changes is to make the average capacity of the Madisonville crania 1338 c. c., instead of 1337 ¢. ¢. Fig. 22. Aboriginal cup, made from a human skull; exhumed near Brookville, Franklin county, Ind. (To illustrate Mr. E. R. Quick’s article in this JOURNAL, vol. iii., pp. 296-297, ) ye : ; i. ee Sd ™ ag Yr. Cee eat Cee eee ae ee Dy ee ee © ee a ee ae ee ee ee a 4 af 258 Cincinnati Society of Natural History. DESCRIPTION. OF A NHW SPECIES OF PAT AND REMARKS UPON A HYALINE By Gro. W. Harper, A.M., Principal of Woodward High School. PATULA BRYANTI, Harper. Fig. 1, dorsal view, magnified 3 diameters; fig. la, ventral view, magnified 3 diameters. Shell broadly and perspectively umbilicate, discoidal, nearly flat above, and deeply excavated below; whorls, five, gradually increasing, regu- larly ribbed, outer whorl bicarinate; color, light brown; aperture, small, rhomboidal; peristome, simple, acute, having its extremities united. Greatest width, 64, least, 54; height, 2 ; width of umbilicus, 44 mill. Habitat, found buried deeply under old logs. Locality, Mitcheli county, North Carolina. | Discovered by A. G. Wetherby, F. W. Bryant, and Geo. W. Harper. Notre.—The above species bears some resemblance to the carinated varieties of the P. perspectiva, and some may consider it a variety of the latter. If it proves to be so, then we are strongly inclined to the opinion that the P. cumberlandiana is only a carinated variety of the P. alternata, as the analogy between the two is very close. Fig. 2. HYALINA SIGNIFICANS, Bland. Fig. 2, dorsal view, magnified 3 diameters; fig. 2a, ventral view, magnified 3 diameters. Shell narrowly, but deeply umbilicated ; pale horn color, epidermis, smooth, shining; whorls, six, increasing slowly, last somewhat in- flated ; irregularly striate, smooth on under side; aperture, lunate; peristome, acute; spire, slightly elevated; base rounded, slightly in- dented around the umbilicus. There are three pairs of pearly teeth within the base of the last whorl, which are plainly seen through the shell. From the peculiar arrangement of the teeth, this shell is readily dis- tinguished from the H. multidentata, as the latter has its teeth arranged in rows of five or six in each row. It isa curious fact that as the H. significans grows old, its teeth gradually disappear. 2 Norre.—This shell was found by Prof. A. G. Wetherby and myself, — while on an exploring expedition in east Tennessee, during the © | I 4 ag Description of New Species of Fossils. 259 summer of 1875. They were found in considerable numbers among the leaves under a little clump of trees in a corn field. The spot was afterward cleared and plowed over, so that this rare shell has become extinct in that locality. The above description differs somewhat from Bland’s original description of the H. stignificans, but the shell we found is undoubtedly the same. DESCRIPTION OF NEW SPECIES OF FOSSILS. By S. A. Mitirr, Esq. TRIGONIA STIEBELI, 0. sp. (Plate VI., fig. 1, view of the left valve; fig. la, cardinal view, the right valve of the specimen is unnaturally inflated.) The shell of this species is very large, subquadrate in outline, and only moderately inflated. The length is a little more than the height. The anterior end extends but slightly beyond the beaks, and is gently rounded below. Nolunule. The beaks are small, anterior, slightly incurved, and raised but little above the hinge line. The hinge line is straight and gently sloping backward. The posterior end is subtruncate above, and rounded into the base below. The base line curves up more rapidly toward the anterior end than behind. About twenty ribs rise from the upper margin behind the beaks, and passing down and curving forward reach the anterior end and basal border. These ribs are very strongly nodulose from the umbonal slope to the anterior and basal margins, and more finely nodulose above the umbonal slope, and between it and the upper margin, though a line of nodules marks the superior border behind the beaks which increase in size toward the posterior end, and another line is directed backward midway between the latter and the umbonal slope. The entire surface of the shell is covered by fine sub-imbricating lines. The specimen illustrated and described was collected by Bernard O. Stiebel, a naturalist, in whose honor I have proposed the specific name, from strata supposed to be of Cretaceous age, in the southeastern part of Arizona. The author, however, is directly indebted to Prof. Ralph Colvin, through whose kindness the specimen was furnished for defini- tion and who also presented it to him. fore el ig A ia 260 Cincinnati Society of Natural History. SACCOCRINUS INFELIX, W. and M. (Plate VI., fig. 2, view of the left side of a cast of a moderately large specimen; fig. 2a, view of the cast of a vault of a small specimen; fig. 2b, shows the appearance near the top of the cup when the plates are preserved.) Megistocrinus infelix, Winchell and Marcy, 1865, Mem, Bost. Soc. Nat. Hist. Body elongated, somewhat pentangularly obpyramidal, and having depressed interbrachial spaces, without any constriction below the arm bases. | Basals wider than high. First radials, the largest plates of the body and a little longer than wide. Second radials, hexagonal and longer than wide. Third radials, heptagonal and longer than wide. First secondary radials, longer than wide. Second secondary radials, about as wide as long and supporting upon the upper sloping sides a single pair of small tertiary radials, which are followed by a single brachial series, and above which the arms become free. Regular interradials, twelve or fourteen; the first is hexagonal, and about the size of the second radials; this is followed by three ranges of two plates each ; a fourth range of three plates ; and a fifth and sixth range of two plates each, the latter“of which are followed by small plates that graduate up through the interbrachial depressions to the top of the vault. There are four or five inter-secondary radials that are followed by small plates, in like manner, to the top of the vault. The azygous area is much depressed in the upper part, though marked by a convex ridge in the middle of the depression, It is covered by numerous plates. The first is heptagonal and equal in size to the first radials. This is succeeded by three smaller plates, and these by others, which are continued over the convex ridge in the depression to the central part of the vault. The vault is flat in the central part, with concave depressions toward the interbrachial spaces at the margin, as shown by a specimen having the plates preserved ; the cast, however, shows the prominent radiating arm furrows as represented by fig. 2a. It is covered by numerous polygonal plates. There are twenty arms. This species is distinguished from S. christyi, with which it has been confounded, by the more elongated form of the body, by the more elongated plates, by the more pointed form at the base, by the more pyramidal and pentangular shape of the body, by the increased number of interbrachial plates, and by the interbrachial depressions. — The latter peculiarity, when the plates are preserved, is alone sufficient Description of New Species of Fossils. 261 to distinguish it. The difficulty in distinguishing a Bridgeport cast from a Waldron specimen covered with plates, does not exist when we have a Bridgeport specimen with the plates preserved to compare with the Waldron specimen. The three specimens illustrated are from the collection of W. C. Egan, Esq., of Chicago, Illinois. He has another specimen with the plates on top of the vault, and those on one side preserved as far down as the top of the third primary radial. CYATHOCRINUS VANHORNEI, D. sp. (Plate VI., fig. 3, view of the left side, also showing the azygous plate—natural size. The lower part of the basal plates on the posterior side have been broken off.) Body strongly constricted at the middle of the sub-radials, and ereatly expanded above on the azygous side. Basals as long, as wide, and the expansion of the cup commencing in the middle part. Sub- radials large, a little longer than wide, hexagonal and pentagonal, and strongly constricted as above remarked. Radials wider than high, and broadly notched for the reception of the arm plates. There is a single large azygous plate resting upon the upper face ofa subradial. The arms are evidently strong, though not preserved in our specimens. Column, unknown. The entire surface of the plates is smooth. The smooth, round, constricted form of the body will distinguish this species from any other. The casts may also be distinguished by the constricted and elongated form. The specimen is named in honor of W. C. Vanhorne, general super- intendent of the Chicago, Milwaukee and St. Paul R. R., a gentleman who finds time to superintend more than 4,000 miles of railroad, and to study the resources, and the geology and paleontology of the whole country traversed by the roads. The specimen illustrated is from the Niagara Group, at Bridgeport, Illinois, and belongs to his fine private collection, at Milwaukee, Wisconsin. GLYPTASTER EGANI, N. sp. } f 4 (Plate VI., fig. 4, side view, natural size; fig. 4a, same view magnified; fig. 40, basal view.) Body of medium size, obpyramidal. Basals small and nearly or quite covered by the column. Subradials well developed, highly con- vex or protuberant with an inclined face directed toward each suture, thus presenting an hexagonal cutting. The first radials almost regu- larly hexagonal, and the largest plates of the body; most highly con- eee ee ee A! eR ey etme bt te 4 4 F sat oe ro 262 Cincinnati Society of Natural History. vex at the upper part where they form a flattened angular ridge, which is continued as the form of the succeeding two radial plates and the secondary radials as far as preserved in our specimen. This ridge bi- furcates toward the subradials below. The second radials are quad- rangular or pentagonal and much wider than high. The third radials are pentagonal or hexagonal, and about as wide as high. Only two or three of the secondary radials are preserved in our specimen. The first regular interradials are nearly as large as the first radials, octagonal, protuberant, and presenting inclined faces toward each of the adjoining sutures. These are followed by two smaller interradials, and these again by two, beyond which our specimen is not preserved. A single intersecondary plate is preserved in our specimen. The protuberant plates and numerous cut faces will alone distinguish this species from any hitherto described. The species is founded upon a single specimen from the collection of W.C. Egan, Esq., in whose honor I have proposed the specific name. It was found in the Niagara Group at Bridgeport, in Chicago, Illinois. LEPERDITIA CACIGENA, 0. Sp. (Plate VI., figs. 5 and 5a, views magnified about five diameters. These two magnified illustrations are not exactly correct, but near enough for all practical purposes. They were drawn without the aid of photographs.) ® Length usually about 12-100 inch, breadth about 8-100 inch. and thickness about 4-100 inch. General form subovate. Hinge line straight, a little more than half the length of the valves. Anterior end narrower than the posterior, extending but little beyond the hinge line, when it rapidly curves into the ventral line below. The posterior part is broadly rounded, and constitutes beyond the hinge-line full one third the length of the valves. Valves most convex at the posterior third. Surface smooth and eye- tubercle obsolete. : This is a true Leperditia, as one valve overlaps the other. - The author collected this species in the upper part of the Hudson River Group at Versailles, and near Osgood, Indiana. The specimens illustrated and described are in his collection. THE JOURNAL OF THE LINGINNATE NIGHETY OF MATURAL HISTORY PROCEEDINGS OF THE SOCIETY, Turspay Evenine, October 4, 1881. Dr. R. M. Byrnes, President, in the chair. Present, 20 members. The Executive Board announced the purchase of the casts of 37 crania, a Glyptodon, and parts of a Mastodon, Dinotherium, Castorot- des ohioensis, Plestosaurus macrocephalus, Ichthyosaurus communis, Hipparion elegans, and Pterodactylus crasstrostris, with the cast of the egg of Apyornis marimus, and some bone implements from the Swiss lake dwellings. Also the skeletons of Pieropus edvardsi, Apteryx oweni, Naja tri- pudians, Uromastrixz spinites, Rana mugiens, Morrhua vulgaris, Raja- batis, and the femur of Loris gracilis. L. $. Cotton made some remarks upon the mountain scenery of Europe and America, and was followed upon the same subject by M. D. Burke and J. R. Challen. . Donations were announced as follows: From Peter G. Thomson, a valuable collection of prehistoric relics, consisting of pottery ware, shell, stone and bone implements, pipes, human remains, etc.: from Joel Brown, a young soft-sheiled turtle; from Dr, A. Gattinger, a specimen of granite; from L. Dressel, a speci- men of Dynastes tityrus ; from J. F. James, fossils, plants and insects from New Harmony, Ind., and minerals from Alabama and Texas; 264 Cincinnati Society of Natural History. from H. G, Hanks, seven volumes on California geology; from Prof. John Collett, Report on Statistics and Geology of Indiana, for 1880 ; from Miss Louisa Dyer, five species of Cincinnati fossils; from C. Faber, twelve species of European and North American fossils; from H. Pugh, one lot pamphlets on mollusca; from Macbrair & Sons, three specimens of lithographic stone; from O. T. Mason, five pamphlets on archeology; from Miss Mary Telfair, one mole skin; from J. M. Patter- son, five volumes of Ohio geology and twenty-six volumes of maps; from Gideon Mabbett, seven specimens alligators and birds’ eggs. Turspay Eventne, November 1, 1881. Dr. R. M. Byrnes, President, in the chair. Present, 18 members. Mr. Davis L. James presented a large fungus (Lycoperdon gigan- teum), commonly known as the “ puff-ball.””. This species, Mr James stated, as well as all others of the genus, is edible; and when properly cooked much resembles in consistency and flavor, an omelet. It should be eaten when only a day or two old, at which time the flesh is firm and pure white. The specimen was ovoid in shape, and measured about ° eight by twelve inches. It was supposed to be less than a week old, and when cut open had a deep lavender color and uninviting appearance. Dr. A. B. Thrasher was elected a regular member of the society. The President announced the recent death of Prof. William Colvin, who had been a prominent and active member of the society for many years. A committee, consisting of Messrs. 8S. A. Miller, 5. E. Wright and L. S. Cotton, was appointed to draft a suitable memorial of his life and services. A committee, consisting of J. A. Warder, U. P. James and 8. T. Carley, was appointed to prepare a tribute to the memory of Mr. John L. Talbott, recently deceased, who was a life member of this society, and a member of the old Western Academy of Natural Sciences. , Mr. A. E. Heighway, Jr., distributed a number of copies of a geological map of Kentucky to the members present. Donations were announced as follows: from the Chief of Engineers, War Department, 14 volumes of valuable Government reports on geology and zoology, etc.; from Dr. R. W. Shufeldt, U. 8. A., two memoirs on Avian Osteology; from Ward and Howell, a cast of a large ammonite; from Jacoh Hoffner, Esq., Cumminsville, Ohio, through Dr. A. E. Heighway, the lower jaw ofa sperm whale, sixteen feet in length; from A. E. Heighway. Jr., a specimen of Calymene niagarensis, from Alabama, and 21 volumes of books and pamphlets on geology; from Dr. A. E. Heighway, a specimen of Sigillaria, from Rockwood, Tennessee; _ from E. O. Hurd, Esq., a specimen of the American bittern, from Alabama; from E. ©, Reiss, a specimen of Bolannus lentiginosus. Turspay Everenine, December 6, 1881. Dr. R. M. Byrnes, President, in the chair. Present, 12 members. Samuel R. Matthews was elected a member. ? Mr, Joseph F. James read a paper on the Variability in the Acorns Proceedings of the Society. =F 26a of Quercus macrocarpa, which is published elsewhere in this number of the JOURNAL. . Mr. S. A. Miller, chairman of the committee, made the following report: The committee appointed to prepare a notice of the life and services of Prof. Wm. Colvin, deceased, and an expression of the esteem in which he was held by this Society, report—— That Wm. Colvin was born near Dumfries, in Scotland, in 1820, graduated at Edinburgh in 1839, and then removed to America with his parents. He located at Pittsburg, Penn., and taught school in the western part of that State for several years. Afterward he was con- nected with the publication of a newspaper, and subsequently was en- gaged for some years as book-keeper for the firm of Hague, Hartupee & Co., engine builders, where he acquired a very thorough knowledge of machinery. About 1850 he formed an Association for the manu- facture of iron, and removed to Ironton, Ohio, where the company con- structed and operated an iron mill until about the year 1855, when he removed to Cincinnati. His taste led him to seek the society of the educated, and the friends of the advancement of science, and he at once became a member of the Western Academy of Sciences. He acted here for some time as agent of the Hanging Rock Mill, and afterward became book-keeper for the Marine Railway and Dry Dock company. During a large part of this time he was President of the Board of Edu- cation of Woodburn, Walnut Hills, where he resided. When this So- ciety was organized he became an active member, and now, as his voice will no more be heard in the discussion of scientific questions, or in the best methods of building up the association so that it will be of the most benefit to us and those who shall draw information from it in the future, we may all unite in acknowledging the valuable services he rendered to the Society, the unselfish zeal manifested in the treatment of all topics in which he took a part, and in eulogizing his kindness and nobleness of purpose. He was secretary of the Society from April, 1874, to April, 1875. In . 1874 he was appointea to the Chair of Political Economy and Civil Polity in the Ohio Agricultural College at Columbus, where he re- mained until 1877, after which time he was engaged in examining and settling up books and examining mineral lands as an expert in regard to their value for coal and iron. Sometime during the last summer he went to Georgia for the pur- pose of exploring and developing some mineral lands. He was taken sick and died of typhoid fever, at Cartersville, on the 26th of October last. His remains were brought to this city, and interred in Spring Grove Cemetery. Those who carried him to his last resting place were Dr. R. M. Byrnes, L. S. Cotton, S. A. Miller, John B. Peaslee, J. S. Taylor, and Chas. A. Thompson. He was distinguished for his honesty and the firmness of his con- victions, His varied experience and habits of study made him a man of great general information, and his close observation of nature and 266 Cincinnatt Society of Natural History. love for natural history made him a naturalist and man of science. Indeed, he was a scholar of no ordinary attainments, and will be missed by the philosophers and thinkers of this city, and his associates in al- most every branch of natural history, where he was always at home in conversation with our best and ablest specialists. He was a friend, a scholar, and a gentleman. S. A. MILER, S. E. Wriceut, } Committee. L. 8. Corron, Mr. V. T. Chambers called attention to the recent death of Prof. J. B. Chickering, and on his motion a committee, consisting of Prof. G. W. Harper, J. W. Hall, Jr., and J. B. Mickelborough, was appointed to draft a suitable testimonial to his memory. Dr. A. J. Howe, in the absence of the chairman of the committee, made the following report: The recent death of Mrs. Abigail Warren recalls to the older mem- bers of the Cincinnati Society of Natural History, the pleasing remem- brance of a generous donation in money, made by the deceased to the Society when it was in its infancy, poor and much in need. This do- nation, when received, called forth a universal expression of thankful- ness, and is still remembered as an important stepping stone in the Society’s progress. We know little of the history of this estimable lady. She was born at Needham, Mass., and after coming to Cincinnati, was married to George Warren, an old and respected citizen, who died several years before her demise. She left no children and no relatives here. The Society has enrolled her name among its honored benefactors. The few members who enjoyed the pleasure of her acquaintance gladly testify to her social eminence, refinement and intelligent benevo- lence, and this Society expresses its sorrow at the demise of its bene- factress, and tenders its sympathy to her surviving relatives. L. S. Corton, A. J. Howe, Committee. J. W. SHORTEN, The following donations were announced: From G. D. Richardson, an illustration of the historical elm tree on Boston Common, upon a thin board made from the wood of the tree; from Mrs, 8S. A. Kendrick, 25 fossils and 16 minerals; from S. T. Carley, a very fine slab of Glypto- crinus decadactylus, and a piece of wood showing borings of the Car- penter bee; from Miss Ellison, ten species of ferns, an Indian tobacco: pouch, some sea weeds and some fossils; from Joseph F. James, the - skin of a snow bird (Junco hyemalis), and eight acorns of Quercus macrocarpa; from Davis L. James, eight species of seeds; from Prof. F. W. Putnam, one volume and two pamphlets on archeology; from the Smithsonian Institution, the proceedings of the U. S. National Museum for 1881; and from the Department of the Interior two volumes and seven pamphlets on Natural History. * ‘Observations on the Unification of Geological Nomenclature, 267 OBSERVATIONS ON THE UNIFICATION OF GEOLOGTI- CAL NOMENCLATURE, WITH SPECIAL REFERENCE TO THE SILURIAN FORMATION OF N. AMERICA.* By 8S. A. Minuer, Esq. The words “system” and “formation” are both in use, in North America, in the nomenclature of the larger geological subdivisions. 4 The former was more generally employed, in the early growth of the science, but is now rarely used, and seems to be gradually growing into disfavor. The latter is preferred, because it is not a technical name, but a word taken in its ordinary signification, and may, there- fore, in general, be omitted. Hence, without fear of being misunder- stood, we speak of the Lower Silurian, or Upper Silurian, or Devonian, without adding the word “formation.” The Silurian includes the entire series of rocks from the base of the Potsdam Group or primordial zone to the Devonian. The Lower Silurian comprises all the rocks from the base of the Potsdam Group to the top of the Hudson River Group. and the Upper Silurian all the rocks from the Hudson River to the Oriskany Group or base of the Devonian. In the nomenclature of any of the lesser geological subdivisions, we do not employ the word “formation,” though, if so employed, it would not necessarily detract from its use, in the nomenclature of the larger subdivisions, because its meaning and force, in the latter case, is too well established to be, in the least, disturbed by other and similar uses. The words series, layer, deposit, bed, zone, horizon, period, age; epoch, and era are used, in geological descriptions, in their literal and ordinary significations. They are not technical names, nor do they _ belong to our geological nomenclature as a necessary part of the system, though they may be very conveniently employed when reference is had to time, as the Mesozoic age, or to the character of the rocks, as the limestone deposits, etc., etc. For the purpose of more definite classification, the Lower Silurian and Upper Silurian have been divided into Groups. A Group gener- ally bears the name of the place where it was first studied and de- scribed. This method of nomenclature is preferred, because the geo- graphical name, when combined with the word “group,” is sufficiently technical; it can not be used for any other purpose, it can never mis- * This article was written at the request of the Committee on the Unification of Geologica Nomenclature, for the International Geological Congress, that held its second session in Bologna, Italy, about the Ist of October last. 268° Cincinnati Society of Natural History. lead as to the mineral or petrological structure or relative position of the strata, and it indicates the typical locality of the exposure. Sandstones and conglomerates of various degrees of fineness, lime- stones of all grades and combinations, shales and marls occur in nearly every group in the Lower Silurian, Upper Silurian, Devonian and Car- boniferous : and, for this reason, geological subdivisions can not be established upon the mineral and petrological characters of the rocks. This has been demonstrated too frequently to demand further consider- ation. The subdivision into groups is founded, substantially, if not entirely, upon the paleeontological characters. The petrography may suggest the subdivision and creation of the group, but its establishment de- pends upon the fossil contents. The fact, however, that the fossils, from contemporaneous animals, must change more or less, in different degrees of latitude, and in deposits made at various depths of the ocean, and be more or less dependent upon the ocean currents that prevailed, and upon the nature of the sea-bottom, which formed their habitat, has rendered it no easy task to determine equivalency of strata, at short distances, and the difficulties and troubles increase as the pe- trographic characters change and distance intervenes. The perplexi- ties thus arising are usually overcome, in proportion to the thickness of the strata, which are understood to constitute the group, the greater or less number of species that have been described from it, the more or less accurate information respecting the grouping of the fossils in its various parts, and the different kinds of rocks in which they are thus grouped or associated. It happens, sometimes, that a group is so de- fined, at one locality, as to show that it is different from any previously defined, and is therefore seemingly worthy to be established ; but afterward, from more complete study and comparison of the fossils, it is ascertained that such group is included, in some manner, within a larger one defined elsewhere, and constitutes part of it, and yet the equivalency of the strata can not be ascertained. In such case, we have synonymy and still both names are usually retained. Again, when groups are separable, and have been separately defined, at one locality as the Medina, Clinton, and Niagara Groups of New York, we find that some authors, describing the series of strata equivalent to these groups, at another place, where they can not be readily dis- tinguished from each other, will propose for them when combined a new name, as the Anticosti Group. Or, perhaps, a better illustration of synonymy of the latter kind is : ; SS See ee he eee Oe See ne oe Observations on the Unification of Geological Nomenclature. 269 found in the use, in nomenclature, of the “Cincinnati Group.” The Trenton, Utica Slate, and Hudson River Groups had been long estab- lished and carefully defined, when some one, supposing, without ex- amination, that the Utica Slate Group did not exist in the vicinity of Cincinnati, and that the rocks belonged either to the Trenton or Hud- son River Groups, or to both, proposed to call the exposure the “ Cin- cinnati Group.” The black slate which characterizes the Utica Slate Group in New York does not exist at Cincinnati, though calcareous slates and shales of the same age do,’ but they so graduate into the Trenton Group below, and the Hudson River above, that the lines of separation have not been accurately ascertained. It is very clear, how- ever, that if the Utica Slate Group had thinned out in its extension westwardly before reaching Cincinnati, there would be no excuse for call- ing the Trenton or Hudson River Group, or both of them together, by a newname, Yet there are some who will persist in using the name “ Cin- cinnati Group,’’ because they don’t know whether it is of the age of the Trenton, Utica Slate, or Hudson River Group, or of the age of all three, and they are bound to leave their readers in the same hopeless confusion. Another kind of synonomy, much more to be deplored, exists, where a group has been named and thoroughly defined, and, for some trivial reason, the geologists of another locality use another name for rocks of the same age without regard to priority in nomenclature. As an illus- tration, the Calciferous Group was established and defined so as to in- clude rocks other than the calciferous sandrock, and ten years after- ward rocks of the same age on the Mississippi river were called the “ Lower Magnesian limestone,” and the Wisconsin geologists persist in the use of the latter name, because they say the word calciferous is not admissible, in that State, from the lithological character of the rock. A reason that has no application whatever, if the foregoing definition of a group is correct, and a reason if carried out, in all cases, would utterly destroy geological nomenclature, for no system can be estab- lished upon lithology. Many other illustrations of synonymy, founded upon like errors of judgment, might be adduced, without including that larger class pro- posed by men who have been employed upon State or Government sur- veys, without the necessary qualifications, and who have suggested names through sheer ignorance and stupidity. These names ought not to be mentioned, even as synonyms, for that is giving to them more _ consideration than they are entitled to receive, and as to many of them more than was required for their publication. x asa Ps oe Ve eae OIE 270 Cincinnati Society of Natural History. The correct rule would seem to be, where a group has been named: and the fossils have been so described and illustrated, that it may be identified elsewhere than at the typical locality, that the law of priority should be rigorously enforced. The larger subdivisions or formations are world wide in their dis- tribution, and it is probable that many of the lesser subdivisions or groups, in distant countries, can be brought into conformity or parallel- ized; but, at present, we can not hope for unification of nomenclature in the latter respect. : Experience has shown the impracticability of making lesser subdi- visions, for the purposes of geological nomenclature,than groups, though it is eminently proper to speak of the marl beds or sandstone layers, in any particular group, or of the Glyptocrinus or Orthis beds, at any particular locality. Such names are used to characterize the strata at the place described, but not in the higher and more extended sense of a geological subdivision. | Passing now from these preliminary observations, we will briefly re- view the distribution, thickness, and paleontological characters, so far as the genera are concerned, of all the groups into which the Silurian has been divided in North America. A complete review of all the paleontological characters would involve an enumeration of 3,560 spe- cific names, and so much minute and dry dissertation that we would have a large book opened up before us, instead of an essay embodying ~ the general facts and the judgment of the writer for special use on this. occasion. THE LOWER SILURIAN. The Lower Silurian is subdivided, in ascending order, into the Pots- dam, Calciferous, Quebec, Chazy, Black River, Trenton, Utica Slate, and Hudson River Groups. There are other groups, having a local ex- istence, that can not be exactly correlated with these, though, no doubt, included within them, which will be mentioned as we progress. In 1838, Prof. Ebenezer Emmons described the petrography of the sandstone, at Potsdam, St. Lawrence county, New York, which he found of considerable thickness, containing fossils, and uniformly overlaid by the Calciferous sandrock of Eaton. He traced it over St. Lawrence and Essex counties, and proposed for it the designation “Potsdam Sandstone.” It was subsequently thoroughiy described in — the New York Reports and other State surveys, and shown to embrace rocks other than sandstones; but it was not until 1863 that it was : Observations on the Unification of Geological Nomenclature. 271 @ fully defined as the Potsdam Group, by showing, as Sir Wm. Logan - did, that it consists of a series of strata, including shale and inter- stratified limestones, as well as conglomerates and sandstone. It has been quite frequently and very properly subdivided into the Upper and Lower Potsdam Groups. The discovery of fossils in strata below the typical sandstone, and the character of the metamorphosed rocks, at the Taconic mountains, led to the attempt to establish the so-called ‘‘ Taconic System.” Prof. Kmmons was certainly correct in many of his discoveries in relation to the order of the strata, but part of his “ Taconic system” evidently be- longs to the Lower Potsdam, and another part to the Quebec Group of the Canadian geologists. In 1865, Prof. Bailey and Mr. C. F. Hartt called an exposure of aren- aceous, argillaceous, and carbonaceous shales, and clay slates often sandy, with sandstone and quartzite, occupying a narrow valley about 30 miles long and 4 miles wide, superimposed to the northwest and northeast upon rocks belonging to the Huronian Group, and having a thickness of about 4,500 feet, near St. John, New Brunswick, the “St. John Group.” These gentlemen, with Mr. Matthew, collected within 200 feet of the base of this great series, fossils which they referred to Paradoxides, Conocephalites, Obolelia, Orthis, Discina, Orthoceras and VYheca, and higher up Lingula. They referred the Group to the primordial fauna, or Htage C. of Barrande, and the Lower Potsdam of America. Subsequently, Prof. Hind referred the rocks to the Que- bec Group, and afterward Prof. Dawson proposed to call them the “ Acadian Group.” While it may be proper to call these deposits the St. John Group, it mever can be, to call them the ‘“ Acadian Group,” if any regard is to be paid to priority in geological nomenclature. The rocks, however, most clearly belong to the Potsdam Group if we are to be governed, in the determination, by the fossils ; for they all belong, so far as they have been determined, to the genera Hocystites, Orthis, Discina, Linguia, Obolella, Theca, Orthoceras, Aynostus, Conocephalites, Microdiscus , and Paradoxides. Hocystites is founded upon a very minute radiated plate, supposed to belong to the order Cysto/dea, an order that reached its greatest development in the Niagara Group, and so far as one may _ be able to judge, such a plate would not be considered remarkable, if found, in any of the groups into which the Silurian has beén divided. Orthis and Orthoceras are genera which extend to the Carboniferous, and occur in all the intervening groups, and are not supposed to 272 Cincinnati Society of Natural History. specially characterize any of them, though Orthoceras reached its most remarkable development in the Black River Group, and Orthis in the Hudson River; Discina and Lingula are genera, probably errone- ously determined, but, if correctly, they have lived in all ages since, and are, therefore, not characteristic of any group. Theca is found in the Potsdam, and continues to occur as high as the Hamilton Group, or Middle Devonian. Agnostus and Conocephalites occur in the Potsdam, Calciferous, and Quebec Groups. Obolella, Paradoxides, and Microdiscus, are Potsdam genera, and possibly indicate that the | strata belong to the Lower Potsdam, While the authors have not re- ferred any of the forms to the species which have been described from _ the Upper Potsdam, nevertheless, there is nothing in the general facies, to distinguish it as a distinct group. Indeed, it would be an extraordinary and notable occurrence to find the same species in the shales and slates at St. John, New Brunswick, and in sandstone at places as distant as Tennessee, New York, and Minnesota, even if they were of precisely the same age. The Potsdam Group, in New York, is usually a hard silicious sand- stone, white, red, gray or yellowish, and having a thickness of from 100 to 200 feet. The lower portion is frequently a granitic conglom- erate, in which masses of rounded and water-worn quartz eight or ten inches in diameter are enveloped. The thickness of this portion is not more than ten feet, but in the extension into Canada it is fully three hundred feet. The sandstone differs in texture and aspect at different exposures. In some places a dark, slaty sandstone, about ten feet in thickness, intervenes between it and the Calciferous; at others, a very coarse brecciated rock intervenes; and, at other places, the passage is | very gradual into the Calciferous sandrock. It extends from New York into Vermont, where its thickness is only from twenty to fifty feet, unless other rocks are included in the group than merely the un-— altered sandstone. It passes from New York into Canada, where it soon attains a thick- — ness ranging from 300 to 700 feet, and, at the summit, the sandstone becomes by degrees interstratified with beds of Magnesian limestone, that constitute a passage to the Calciferous. It rests unconformably — upon and fills up the inequalities of the underlying Laurentian forma- tion over a great part of the area of its distribution. Below the Chau-— diere, it consists, at the base, of red, green, black, and lead-gray shales, — and hard arenaceous-calcareous argillites, interstratified with eray sandstones, and of gray limestone and limestone conglomerates, inter-— img Observations on the Unification of Geological Nomenclature. 273 we stratified with black limestones, and black shales, and gray sandstones having a thickness of 700 feet; succeeded by gray sandstones inter- stratified with black and gray argillo-arenaceous shales, and calcareo- arenaceous bands, and sometimes conglomerates, 700 feet; and this series is followed by 600 feet of conglomerate, holding limestone and quartz pebbles interstratified with black shale, slightly arenaceous; and a gray quartzose sandstone holding flakes of black and greenish shale, and occasional pebbles of limestone; making a total thickness of 2,000 feet. The ever-varying character of the strata may be observed in its ex- tension to the extreme eastern part of the continent, at Belle Isle, and New Foundland, and likewise westerly, by the way of Lake Huron and the Lake Superior region, across Wisconsin and far into Minnesota. In the vicinity of the trappean rocks of Lake Superior, where volcanic agencies are evident, it attains a thickness of 5,000 feet, and often consists of conglomerates composed of trappean pebbles cemented by a volcanic sand. In other places, it consists of white silicious sand, enveloping pebbles of quartz and patches of slate; and again it has a deep red color, and contains patches of dove-colored clay. It “never exhibits, in long distances, a homogeneity of structure, or uni- _ formity in thickness, and not unfrequently it takes into its composti- tion, in the upper part, particles of lime, and finally graduates into the overlying Calciferous. . It has an enormous development in the Appalachian mountains, and : particularly in Tennessee, where it consists, at the base, of coarse, eray conglomerates, talcose, chlorite and clay slates, interstratified, and having a semi-metamorphic aspect, and a thickness of 10,000 feet. In some places the conglomerate predominates over the slates, and has a thickness alone of 6,600 feet. This great thickness is succeeded by heavy-bedded sandstones, sometimes having sandy shales and thin flags interstratified, and containing scales of mica, and at other times green grains of glauconite; thickness, 2,000 feet. This is followed by bard, brown, greenish and gray shales, and thin sandstones, interstrati- fied with which are several layers of hard, dark, gray sandstone, the whole being 1,000 feet thick; this by soft variegated shales 2,000 feet _ thick; and this again by a heavy series of dolomites and limestones, 4,000 feet in thickness; making a total thickness of 19,000 feet. Inter- _ stratified with the variegated shales, at intervals, are layers of blue limestone, which are often oolitic, and sometimes fossiliferous. It is well exposed in Missouri, Texas, and many places in the Rocky +k ie 274. Cincinnati Society of Natural History. Mountain region, where it presents the usual variety of lithological char- acters. In some localities it is a conglomerate of more or less water-worn pebbles, mostly whitish crystalline quartz, and varying from 2th to 4 inches in diameter, cemented together with a silicious paste. Some of the pebbles are scarcely worn, while others are quite smooth. At other places, the sandstone contains micaceous particles, and often calcareous matter, and sometimes seams occur from 2 to 4 inches in thickness, almost entirely composed of Obolella and Linguloid shells. This Group contains ripple marks, wave lines, mud cracks, animal tracks and worm burrows, but such things occur even to the present day, though we distinguish the Potsdam tracks by the names Climach- tichnites and Protichnites, and the burrows by Scolithus, a generic name, which is also applied to fossils in the Hudson River and Medina Groups. And there are Veretts, Myrianites, and Nemapodia, of un- certain affinity. In the vegetable kingdom, we have Palewophycus, which occurs in the Calciferous, Hudson River, Medina, Clinton, and as high as the Coal Measures; Buthotrephis, which occurs in the Calciferous, Trenton, Utica Slate, Hudson River, Clinton, and Waterlime Groups; Arthraria, which occurs in the Trenton and Hudson River; and Hophyton and Cruziana which are peculiar to it. The Protista are represented by Archeocyathus, which occurs in the | Calciferous, and Protocyathus which is peculiar to it. | The Polypi are represented by Dendrograptus; which occurs in the Quebec, Utica Slate, Hudson River, and Niagara Groups; and Old- | hamia, which occurs in the Trenton. The Echinodermata are represented only by Hocystites above men- | tioned. } The Brachiopoda are represented by Orthis, Obolella, Discina and — Lingula, as above mentioned; by Crania and Orthisina which occur in the Calciferous, Trenton, Hudson River, and other Groups as high as the Coal Measures; by Leptena which occurs in the Trenton, Utica : Slate, Hudson River, Clinton, Lower Helderberg, and Oriskany Groups; by Camarella, which occurs in the Calciferous, Quebec, Chazy, Black River, Trenton, Hudson River, and Clinton Groups; by Lingulella and Trematis, which occur in the Trenton and Hudson River: by Lin- gulepis, which occurs in the Chazy; by Acrotreta and Iphidea which occur in the Quebec; and by Kutorgina, which alone is peculiar to it. The Pteropoda are represented hy Theca, as above mentioned; by — Hyolithes, which extends to the Hamilton, and by Hyolithellus, which | | is peculiar to it. : | Observations on the Unification of Geological Nomenclature, 275 The Gasteropoda are represented by Bellerophon, Platyceras, Pleu- rotomaria and Straparollus, which occur in every group as high as the Coal Measures. Pleurotomaria canadensis is known as a species to pass up into the Calciferous. By Holopea, which occurs in every group to the Warsaw in the Subcarboniferous; by Ophileta which oc- curs in the Calciferous, Quebec, Trenton and Galena; by Straparollina, which occurs in the Quebec and Black River Groups; and by Paleac- mea which alone is peculiar to it. The Cephalopoda are represented only by Orthoceras as above men- tioned. The Annelida are represented by Serpulites, which is accredited to the Chazy, Trenton and other groups as high as the Coal Measures. and by Salterella, which occurs in the Trenton. The Crustacea are represented by Agnostus, Conocephalites, Micro- discus, and Paradowxides, above mentioned; by Leperditia, which oc- curs in the Calciferous, Quebec, Chazy, Trenton, Utica Slate, Hudson River, Clinton, Niagara, and on to the Carboniferous; by Bathyurus, which occurs in the Calciferous, Quebec, Chazy, Black River and Tren- ton; by Amphion and Arionellus, which occur in the Calciferous, Quebec and Chazy; by Bathyurellus, Bathynotus, Crepicephalus, Pthychaspis, Olenellus, and Menocephalus, which occur in the Quebec; by Jilenurus, which occurs in the Calciferous; and by Aglaspis, Ag- raulos, Anopolenus, Chariocephalus, Conocoryphe, Pemphigaspis, So- lenopleura, and Triarthrella, which are peculiar to it. It thus appears that less than one third of the genera found within the whole range of rocks, which intervene between the metamorphosed Huronian series and the Calciferous, that have been included in the Potsdam group, are unknown in later times ; more than one third pass up into higher groups, but not beyond the Lower Silurian; of the re- mainder, a few became extinct in the Upper Silurian, a few in the Devonian, and the rest amounting to about twenty per cent. occur in the Carboniferous, and some in later formations. Or, in other words, more than two thirds of the genera known from the Potsdam occur in higher groups, and it is linked specifically with ° the succeeding Calciferous as well as graduating into it as above stated. There is nothing in the thickness, structure or fossil contents as it spreads over the States from the Appalachian mountains, that demands a subdivision beyond the provisional one of Upper and Lower Potsdam, and within the mountain districts, where it is found in such enormous thickness, it has not been separated into groups by satisfactory defini- see ee 276 Cincinnati Society of Natural History. tion. Nor can there be any argument drawn from the distribution of the fossils, that will separate it from other Lower Silurian groups by stronger lines than those which distinguish groups in other formations. The word “Cambrian,” in its application to this group is not ad- missible, because it is part of the Lower Silurian. Beside, the word ‘Cambrian,’ for want of proper definition, ranks for uncertainty, even in England and Wales, with the word “Taconic” in America. There are some who use such mongrel names as “Cambro-Silurian” and “ Siluro-Cambrian,” which have about as accurate significance, in geological nomenclature, as Cretaceo-Pliocene would have, or as Orthocero-Calymene would have in paleontology, if one should apply it to a trilobite found within an Orthoceras, or Platycero-Goniasterot- docrinus appled to a Platyceras attached to the vault of a crinoid. Or, a better illustration still, in order to settle all questions relating to Chetetes and Monticulipora just call the names Monticuliporo-Che- tetes, or Cheteto-Monticulipora. How absurd! The Calciferous Group.—This group was first defined by Lardner Vanuxem, in 1842, in the Geology of the Third District of New York. He defined and united into one division, the silicious layers above the Potsdam sandstone, with the “ Calciferous sandrock” or “ Transition rock,’ of Prof. Eaton, and the “Bark-like layers” of Eaton, or ‘‘ Fu- codial” layers of the early New York geologists, under the name of the Calciferous Group. fn New York, the lower part is compact and silicious, and graduates into the Potsdam below, the middle part is a sandy limestone having a shattered appearance, and the upper part is apparently a mixture of calciferous material with compact limestone. The thickness is from 250 to 300 feet. It extends from New Jersey across New York into Vermont, where the prevailing character is that of a sandy limestone, compact and thickbedded, and having a thickness in the broken up mountain ranges of 300 feet. From New York it extends into Canada, where it is, generally, a granular magnesian limestone, covers several thousand square miles, and reaches a thickness of 450 feet. It occurs on the Mingan Islands, 500 or 600 miles to the northeast, and is finely exposed in Newfoundland, where it consists of definitely stratified limestone having a thickness of 2,000 feet or more. It occurs in the Lake Superior region, on the St. Mary’s, Escanaba and Menomonee rivers, and extends westerly across the State of Wis- consin into Minnesota. It is seen in the bluffs of the Mississippi, from the Falls of St. Anthony to the mouth of the Wisconsin river. le The thickness near the head of Lake Pepin is 185 feet, but south a few hundred miles in the State of Missouri it expands to a thickness of 1,300 feet. It exposes a thickness in northwestern Texas of about 400 feet, and occurs at many other places in the far west. The genera which are first known to make their appearance in this eroup, are distributed as follows: Among the Protista, Calathiwm occurs in the Quebec and Chazy; feceptaculites in the Trenton, Hudson River and Niagara; hab- daria, Ribeira, and Trichospongia, are peculiar to it. Among the Polypi, Monticulipora occurs in the Chazy, Trenton, Utica Slate, Hudson River, Clinton, and as high as the Devonian. Among the Gasteropoda, Huomphalus, Murchisonia, and Metop- toma, occur in almost every succeeding group to the Coal Measures; Subulites in every group to the Guelph; Trochonema and Helicotoma occur as high as the Upper Helderberg; Hunema occurs in the Black River and Niagara; Maclurea occurs in the Quebec, Chazy, Black River and Trenton; and Scevogyra is peculiar to it. Among the Cephalopoda, P2loceras occurs in the Quebec. Among the Lamellibranchiata, a class unknown in older rocks, Cypricardites occurs in nearly every succeeding group to the Carbon- iferous ; and Huchasma occurs in the Quebec. Among the Crustacea, Dolichometopus occurs in the Quebec. Of the nineteen genera mentioned, four are peculiar to the Calcifer- ous, five pass into higher groups, but not beyond the Lower Silurian, three terminate in the Upper Silurian, three in the Devonian, and four in the Carboniferous. This group is connected with the Quebec by numerous species, which occur in both, among which are Ophileta uniangulata, Holopea dili- cula, Helicotoma perstriata, Pleurotomaria caicifera, P. postumia. Maclurea matutina, M. sordida, Ecculiomphalus canadensis, Camar- ella calcifera, Lingula mantelli, L. irene, Amphion salteri, Bathyurus cordat, B. conicus, and Asaphus canalis, the latter also occurring in the Chazy. It, also, so graduates into the Quebec, at some localities, that no distinguishing line of separation has been observed. The Quebec Group.—This group was first characterized, and its. position between the Calciferous and Chazy determined, by Prof. E. Billings, in 1862. It was further defined in 18638, in the Geology of Canada, and its fossils afterward more fully described by Prof. Hall, in Decade II. of the Survey of Canada, and by Prof. Billings in his Palzeozoic Fossils. 278 Cincinnati Society of Natural History. With the exception of a small portion on the north shore, between Cape Rouge and Quebec, and part of the island of Orleans, itis en- tirely confined to the south side of the St. Lawrence ; where its north- western limit occurs between Missisquoi Bay and Cape Rouge; and southeastern limit is traced from Stanstead, east of Lake Massawippi, to St. Francis river, and along this river to Lake St. Francis. From this the southern boundary is traced to Vandreuil, on the Chaudiere ; thence to the northern part of Lake Temisconata, and following the province line to Lake Metis. It then stretches eastward to the ex- remity of the continent at Cape Rosier. It reaches its greatest breadth on the Chaudiere, which is about sixty miles. It forms the continua- tion of the Green Mountains of Vermont, and includes in Canada the Shickshock and Notre Dame Mountains, and has a thickness estimated at more than 12,000 feet. Part of it may belong to the upper part of the Calciferous, and another part to the Chazy, but it is exposed only in a region much disturbed by volcanic action, and how much if any of it is synchronous with other groups may never be known. The Chazy, when found superimposed upon the Calciferous, is al- ways uncomformable, but when the Quebec intervenes, the connection is shown by the gradual change in the fossils from the Potsdam and Calciferous below to the Chazy and Trenton above. The genera, so far as known, that make their first appearance in this group, are distributed as follows : Among the Protista, Zrachyum is peculiar to it. Among the Polypi, Callograptus and Ptilograptus, recur in the Niagara; Thamnograptus in the Hudson River and Niagara ; Dictyo- nema in the Trenton, Niagara and Hamilton Groups ; Graptolithus and Retiolites in the Clinton ;'Climacograptus, Diplograptus and Retiograptus, in the Trenton, Utica Slate and Hudson River; while Cladograptus, Dawsonia, Didymograptus, Discophyllum, Monograp- tus, Nemagraptus, Nereograptus, Phyllograptus, Staurograptus, and Tetragraptus, are peculiar to it. Among the Echinodermata, Stenaster occurs in the Trenton and Hudson River ; and Palewocystites in the Chazy. Among the Brachiopoda, Strophomena occurs in every succeeding group to the Devonian ; Stricklandinia in the Clinton and Niagara ; and Porambonites in the Black River Group. Among the Gasteropoda, Cyrtolites and Metoptoma occur as high | as the Carboniferous ; Cyclonema, as high as the Devonian; Fusis- pira, in the Trenton, Utica Slate, and Hudson River; and Clisospira and Ecculiomphalus in the Trenton. Observations on the Unification of Geological Nomenclature. 279 Among the Cephalopoda, Nautilus is a living genus, though it should be considered doubtful as to identification in such remote ages; Oyrtoceras occurs in every group to the Coal Measures; Trochoceras to the Devonian; ZLituctes to the Niagara; Hndoceras to the Hudson River; and Cyrtocerina to the Black River Group. Among the Lamellibranchiata, Yellinomya occurs in the Black River, Trenton, Hudson River, and. as high as the Devonian; and Eopteria if distinct trom Huchasma is peculiar to it. Among the Crustacea, Beyrichia occurs in every group to the Coal Measures; Lichas occurs in the Chazy, Black River, Trenton, Hudson River, Niagara, and Lower Helderberg; Jllenus, Cerauerus, and Encrinurus, in the Chazy, Black River, 'Trenton, Hudson River, Clinton and Niagara; Harpes and Asaphus in the Chazy, Trenton, Utica Slate and Hudson River; QOlenus in the Hudson River; Yriarthrus in the Utica Slate; Remopleurides in the Chazy and Trenton; Ampyzx in the Chazy; and Hndymionia, Harpides, Holometopus, Megalaspis, Ni- deus, Ogygia, Shumardia, and Telephus, are peculiar to it. Of the fifty-seven genera that are thus supposed to have commenced their career in this group, twenty did not pass beyond it, but ten of these are Graptolitide, a family that commenced an existence in the Potsdam, and reached the climax of its evolution in this group, and declined gradually, thereafter, though the largest known form existed in the Hudson River Group. Eight of the remaining ten belong to the Trilobites, an order that flourished in the Potsdam, and was in the height of its evolution in this age, but continued to survive until near the close of Palzeozoic time. Seventeen of the genera passed into higher groups, but not beyond the Lower Silurian; ten became extinct in the Upper Silurian; five in the Devonian; four in the Carboniferous; and one is supposed to have survived all vicissitudes to the present time. It is connected specifically with higher groups by Maclurea atlan- ¢ica, which passes up into the Chazy; and by Leptena sericea, which occurs inthe Chazy, Black River, Trenton, Utica Slate, Hudson River, and Clinton. The limits of the group are still a subject of discussion, but the existenve of it between the Calciferous and Chazy, seems to be firmly established. The Chazy Group.—In 1842, Prof. Emmons defined this group under the name of the “Chazy limestone.” The name is derived from the town of Chazy, in New York, where he found it well exposed be- tween the Calciferous and Birdseye limestone, and having a thickness 280 Cincinnati Society of Natural History. of 130 feet. It consists of a dark, irregular, thick-bedded limestone, sometimes containing rough, flinty or cherty masses. It crosses over into Vermont, where it covers more surface than any other group of the Lower Silurian, and has a thickness of 300 feet. In 1863, the Canadian geologists, finding the limestone associated with shales and sandstones, called it the “ Chazy formation.” It covers a considerable area in Canada, reaching as far as the Mingan Islands, and sometimes exposing a thickness of 300 feet. It appears in the Lake Superior region where the bottom layers are arenaceous, and higher up they have an argillo-calcareous composition. It extends westwardly across the State of Wisconsin into Minnesota, where it is usually a quartzose, incoherent sandstone, and bears the name of the St. Peters sandstone, from its development on a river of that name. In this region it fills the deep hoitlows that had been worn out of the Calciferous group before its deposition. It sometimes varies from a foot or less to 200 feet or more in thickness, within a very short dis- tance—the variation of a hundred feet not unfrequently taking place within a quarter of a mile. In Tennessee, it consists of a blue, more or less, argillaceous lime- stone, having a thickness of 600 feet, succeeded by red and gray marble, valuable for building and ornamental purposes, 400 feet in thickness. It occurs in Missouri, Nevada, Utah and other places in the Rocky Mountain region. Though a group of no very great thick- ness, it has an extensive geographical range, and in some places is quite fossiliferous. In New York it so graduates into the Birdseye limestone that constitutes the base of the Black River Group, that some of the early geologists united them into one group. The genera, whose appearance is first known in this group, are dis- tributed as follows : Among the plants, Rusophycus occurs in the Black River, Trenton, Hudson River, and Clinton Groups. Among the Protista, Hospongia is peculiar to it. Among the Polypi, Streptelasma and Columnaria occur in the Black River, Trenton, Hudson River, Clinton and Niagara; and Bolboporites is peculiar to it. Among the Echinodermata, Rhodocrinus recurs in various groups as high as the Carboniferous; Hybocrinus, Palewocrinus, and Glyptocys- tites occur in the Trenton; and Blastoidocrinus, Malocystites and Pachycrinus are peculiar to it. Among the Bryozoa, Fenestella occurs in nearly every group as high as the Coal Measures; and Stictopora in every group to the Devonian. Re one 3 2 4 ieee bad Batali Bali Peas mie: Ra Observations on the Unification of Geological Nomenclature. 281 Among the Brachiopoda, Rhynchonella occurs in nearly every group to modern time. Among the Gasteropoda, Capulus extends to the Coal Measures; Bucania to the Lower Helderberg; Raphistoma to the Niagara; and Scalites to the Trenton. Among the Cephalopoda, Actinoceras extends to the Carboniferous; Oncoceras to the Niagara; and Ormoceras to the Clinton. Among the Lamellibranchiata, Modiolopsis to the Lower Helderberg; and Ambonychia to the Niagara. Among the Crustacea, Spherexochus occurs in the Black River and _ Niagara Groups. Of the 24 genera that come into an existence in this group, five do not pass beyond it; four terminate in groups belonging to the Lower Silurian; nine in the Upper Silurian; one in the Devonian; four in the Carboniferous; and one has existed through all succeeding time. This group not only graduates lithologically into the Black River, but it is connected intimately by numerous species, some of which pass into the Trenton and Hudson River Groups. Strophomena alternata, and S. tncrassata, pass up into the Hudson River; and Orthis borealis, O, disparilis, O. perveta, Leperditia canadensis, L. louckana, L. amygda- dina, Orthoceras multicameratum, O. bilineatum, Modiolopsis nasuta, are among those that pass up into the Trenton Group. The separation from the Black River is however very marked where the passage beds formed by the Birdseye limestone do not intervene. The Black River Group.—This Group was defined by Lardner Van- uxem in 1842, and named from Black River, New York. It includes the Birdseye and Black River limestones. The Birdseye received its name from the crystalline spots of a species of Tetradium, and a fucoid, which areshown when the rock is fractured. It is distinguished by its _ light dove color, thick layers, and vertical joints. It is foand in Essex, Clinton, Lewis, and Jefferson counties, New York, having a thickness of 30 feet. It has been identified in a few other places in the State and alsoin Vermont, but in Canada it has become so united with other strata, that no line of separation can be determined. Phytopsis, Stromatocerium, Tetradium, Orthostoma, and Colpoceras are genera that appear for the first time in the Birdseye limestone, but all of them occur in the Black River limestone, Colpoceras occurs also in the Trenton, and Tetradium in the Trenton and Hudson River, and as so many species range into the Black River limestone, there is not sufficient reason for ranking it higher than beds of passage forming the lower part of the Black River Group. 282 Cincinnati Society of Natural History. The Black River limestone in New York is usually a gray, compact or subcrystalline limestone, or blue compact limestone, and distin- guished by the remarkably large specimens of Orthoceras that occur in it. Some of them are ten feet in length, and a foot in diameter. The thickness is about 50 feet. In Vermont it constitutes the black marble of Isle La Motte, where its thickness is from 12 to 20 feet. . The Group spreads over quite an extensive area in Canada, rarely attaining any great thickness, though on the St. Lawrence 90 miles be- low Quebec, it has a thickness of 136 feet. Its existence has been noted in the Lake Superior region on St. Mary’s, Escanaba, and Me- nomonee rivers, on St. Joseph and Sugar islands, and at Plattsville, Wisconsin. In Missouri, it forms exposures 75 feet in thickness. In Pennsylvania, it is said to have very great thickness, but the geological surveys of that State have been so poor, and so much worthless syn- onymy has been injected into the reports that one can not acquire much information about its geology without personal examination, or with- out waiting until after a geological survey shall be organized anew. The distribution of the genera which commence an existence in this eroup is as follows: In the vegetable kingdom, Licrophycus occurs in the Trenton and Hudson River, and Phytopsis is peculiar to it. Among the Protista, Astylospongia occurs in the Trenton and Niagara, and Stromatocerium in the Trenton. Among the Polypi, Stromatopora and Petrata occur in succeeding » eroups as high as the Devonian; Calapecia occurs in the Hudson River and Clinton, and Yetradium in the Trenton and Hudson River. Among the Brachiopoda, Streptorhynchus occurs in nearly every succeeding group to the Permian; Dinobolus occurs in the Guelph; and Hichwaldia in the Niagara. Among the Pteropoda, Pterotheca occurs in the Trenton and Hud- son River. Among the Gasteropoda Loxonema occurs as high as the Permian; Hunema as high as the Devonian, and Orthostoma is peculiar to it. Among the Cephalopoda Gyroceras and Phragmoceras occur in various groups to the Subcarboniferous; Gomphoceras occurs as high as the Hamilton; Colpoceras and Gonioceras occur in the Trenton; and Conoceras is peculiar to it. Among the Lamellibranchiata, Conocardium occurs in various groups as high as the Subcarboniferous, and Lyrodesma occurs in the Trenton and Hudson River. a Observations on the Unification of Geological Nomenclature. 283 Among the Crustacea, Jsochilina occurs in the Trenton, Hudson River, and Medina, and Cytherina and Cytheropsis in the Trenton. Of the 25 genera thus enumerated as commencing an existenc2 in this group, only three are peculiar to it; eight become extinct in the Trenton and Hudson River; five in the Upper Silurian; four in the Devonian; and five in the Carboniferous and Permian. This group is especially distinguished for the wonderful evolution of the Cephalopoda which it presents. One fifth of all the genera belonging to this class in the Paleozoic rocks came into existence in this group. One genus commenced and terminated its existence, and the family Orthoceratide that commenced its career in the Potsdam passed its period of greatest development here, though some species survived until the age of the Coal Measures. The Trenton Group.—This group was named from Trenton, Oneida county, New York. The limestone, at Trenton Falls, where it is over 100 feet in thickness, was called the “ Trenton limestone,’ long prior to the use of the words in a geological sense. In 1838, Lardner Van- uxem referred to the Trenton limestone, but it was not until 1842 that he and Prof. Emmons so defined the group as to fully establish it. At Trenton Falls, it consists, in the lower part, of a dark-colored, fine-grained limestone in thin layers, separated by black shale or slate, which forms the great mass through which the creek has worn its channel, and in which are all the falls; the upper part is a gray, coarse- erained limestone in thick layers. It is finely developed in Lewis, Oneida, Herkimer and Montgomery counties, where its thickness is about 300 feet, and still more extensive in Clinton and Jefferson counties, where it has a thickness of 400 feet. It also occurs in other counties of the State. In Vermont there are three narrow outcrops, consisting of black schistose layers, associated with slaty seams of limestone, and occasional argillaceous matter, having a thickness of about 400 feet. It has an extensive geographical distribution in Cana- da. The Montreal, Bay St. Paul, and Ottawa sections have, each, a thickness of 600 feet. The sections in western Canada, on the Trent river, and at Collingwood, have a thickness of more than 750 feet. It is much thinner farther west in Wisconsin and Minnesota. In Missouri it is more than 300 feet thick. In eastern Tennessee it consists, at the base, of a highly ferruginous sandy limestone, having a thickness of 700 feet, followed with flaggy limestone and calcareous shale, 800 feet thick, and this again by variegated marble 300 feet. In middle Tennessee, and central Kentucky, the thickness is about 500 feet. The 284 Cincinnati Society of Natural History. Galena limestone of Illinois, lowa and Wisconsin, belongs to the upper part of this group. It is found almost everywhere on the continent where Lower Silurian rocks are exposed, and in all cases is very fossil- iferous, The distribution of the genera that are first observed in this group is as follows: . Among the Protista, Beatricea passes up to the Clinton; Pasceolus to the Hudson River: and Brachiospongia and Cnemidium are peculiar to it. Among the Polypi, Aulopora passes up through the Upper Silurian and Devonian : Paleophyllum, Protarea and Stellipora to the Hud- son River; and Buthograptus is peculiar to it. Among the Echinodermata, Agelacrinus passes up to the Subcarbon- iferous ; Homocrinus, and Paleaster to the Devonian; Thysanocrinus, Petraster, Lecanocrinus, Glyptocrinus, and Dendrocrinus to the Ni- agara; Carabocrinus, Cyclocystoides, Heterocrinus, Lichenocrinus, Paleasterina, Pleurocystites, Porocrinus, and Retiocrinus to the Hud- son River; and Amygdalocystites, Ateleocystites, Cleiocrinus, Co- marocystites, Edrioaster, Hybocystites, Schizocrinus, Scyphocrinus, Syringocrinus, and Teniaster are peculiar to it. Among the Bryozoa, Ptilodictya passes up to the Coal Measures ; Alecto, Ceramopora, Clathroporo, and Retepora, to the Devonian ; Escharopora, Paleschara, and Phenopora to the Upper Silurian ; Bythopora to the Hudson River, and Arthroclema is peculiar to it. Among the Brachiopoda, Atrypa and Pholidops pass up to the De- vonian; and Zygospira and Rhynchotreta to the Lower Helderberg. Among the Pteropoda, Conularia passes up to the Kaskaskia Group of the Subcarboniferous, and Zentaculites to the Chemung. Among the Gasteropoda, Carinaropsis, Cyclora and Microceras pass up into the Hudson River, and Conchopeltis is peculiar to it. Among the Cephalopoda, Z'rocholites passes into the Hudson River. Among the Lamellibranchiata, Pterinea and Cypricardinia pass up to the Carboniferous; Cleidophorus to the Niagara; and Matheria is peculiar to it. Among the Annelida, Cornulites passes up to the Devonian. Among the Crustacea, Calymene and Dalmanites pass up to the De- vonian; Acidaspis and Bronteus to the Lower Helderberg; and T'rinu- cleus and Sphaerocoryphe to the Hudson River. Of the 67 genera thus enumerated as commencing their existence in this Group, 19 terminated in the Hudson River, 14 in the Upper Sil-: urian, 13 in the Devonian, 5 in the Carboniferous, and the remaining — Observations on the Unification of Geological Nomenclature. 285 16 terminated their career within it. Streptorhynchus filitextum, Asa- phus gigas, Calymene callicephala, Rhynchonella capax, and numer- ous other species, pass up into the Hudson River; while Zygospira modesta, and Strophomena tenuistriata pass on into the Upper Silurian. The Utica Slate Group.—This Group was named from its exposure at Utica, New York, and was defined, in 1842, by both Lardner Van- uxem and Prof. Emmons. It extends from New Jersey, across the State of New York, into Vermont, and passing under Lake Champlain enters Canada, where it spreads over a large area to the north and east, and extends westerly from Lake Ontario to Lake Huron. It is through- out a dark colored slate, loaded with carbonaceous matter. It is inter- stratified with thin bands of limestone, and passes into the Trenton Group below by gradual interstratification. In some places the lam- ine are coated with a thin film of anthracite, and in other places sili- cious slate occurs of red, green, brown and black colors. In New York it reaches a thickness of 250 feet; in Vermont, 100 feet; in Can- ada, 510 feet; and in Pennsylvania, 400 feet. It thins out westerly, and while it separates the Trenton and Hudson River Groups at Cin- cinnati, on the Ohio river, it has lost its character of a black slate, and is composed of blue calcareous shales and marls, with interstratified thin limestones. and apparently forms mere passage beds from the Trenton to the Hudson River Groups. The distribution of the genera which commence an existence in this group is as follows: In the vegetable kingdom, Cyathophycus and Discophycus are pe- culiar to it. Among the Brachiopoda, Zeptobolus and Schizocrania pass up into the Hudson River. And among the Crustacea, Plumulites passes up into the Hudson River. Of the five genera thus supposed to commence their existence in this group, two do not pass beyond it, and the other three become extinct in the Hudson River. While many of the Trenton species pass through it, yet there are a number which are characteristic of it, among which is 7'riarthrus becki, a species that follows the group in its extended geographical distribu- tion, and changes of character, but is not known in either older or younger strata. The Hudson River Group.—This group was named from the ex- posure on Hudson river, in New York, and first defined, in 1842, by Lardner Vanuxem. In New York it consists of shales, shaly sand- stones, sandstones, slates and thick-bedded grits. The slates and 286 Cincinnati Society of Natural History. shales are generally dark brown, blue and black, and the grits gray, greenish and bluish gray. They are stratified and conformable, alter- nating a great many times without any regular order of alternation. The thickness is about 800 feet. It has a wide geographical distribu- tion in Canada, and reaches a thickness of 2,000 feet. In the Lake Huron region it consists of a bluish or greenish colored argillaceous shale, holding thin beds of dark blue argillaceous, yellow-weathering sandstone; near the top there are marls, which are red, green, or a mixture of both: they hold very thin beds of dark bluish argillaceous limestone, the whole being surmounted by beds of gray or bluish aren- aceous limestone. The thickness on Grand Manitoulin Island is 200 feet. In Ohio, Indiana and Kentucky, it consists of irregularly alter- nating layers of calcareous shale, marl and limestone. The thickness is about 800 feet, and the upper part is extremely fossiliferous. It occurs in Pennsylvania, Virginia, Tennessee, Missouri, Iowa, Texas, and New Mexico, and may be regarded as a universal group, though its petrological characters change, essentially, at distant localities. The fossils are, usually, remarkably well preserved and abundant, and we are, therefore, frequently able to identify species that commenced an existence in earlier groups. ‘There are many peculiar tracks found on the indurated shales supposed to have been made by Gasteropoda, Cephalopoda and Trilobites that have received such generic names as Asaphoidichnus, Trachomatichnus, Teratichnus, Petalichnus, Orma- thichnus, and Serichnites. The distribution of the other genera supposed to have commenced their existence in this group is as follows: In the vegetable kingdom, Blastophycus, Heliophycus, Dystacto- phycus, Dactylophycus, Trichophycus, and Sphenothallus, are peculiar to it. Among the Protista, Microspongia is peculiar to it. Among the Polypi, #istulipora, Zaphrentis, and Favosites pass up to the Carboniferous; Alveolites to the Devonian; Halysites, Helio- lites, and Sarcinula to the Niagara: Favistella to the Clinton; and Megaloyraptus, Dicranograptus, and Columnopora are peculiar to it, Among the Echinodermata, Protaster passes up to the Keokuk Group of the Subcarboniferous; Anomalocystites to the Oriskany; Lepadocrinus to the Lower Helderberg; Hemicystites to the Niagara; and Anomalocrinus, and Xenocrinus are peculiar to it. Among the Bryozoa, Cyclopora and Trematopora to the Subcarbon- iferous. “pa? Sra) oe. ee ee a ee a A, i Observations on the Unification of Geological Nomenclature, 287 Among the Brachiopoda, Trematospira to the Hamilton. Among the Gasteropoda, Phragmostoma to the Hamilton. Among the Cephalopoda, Ascoceras passes up to the Clinton. Among the Lamellibranchiata, Sedywickia and Orthonota pass to the Carboniferous; Anodontopsis to the Devonian; Lschyrinia to the Clin- ton; and Anomalodonta, Cuneamya, Cycloconcha, Angellum and Orthodesma are peculiar to it. Among the supposed Annelida, Spirorbis extends to the Coal Measures; and Nereidavus and Walcottia are peculiar to it. Among the Crustacea, Cythere passes up through the Coal Measures, and Proetus to the Carboniferous. Of the 43 genera (without including tracks) thus enumerated, as commencing in this group, 19 do not pass beyond it; six become ex- tinct in the Upper Silurian, five in the Devonian, and the remaining eleven pass up into the Carboniferous. With this group, we close the Lower Silurian Formation, because we have here the greatest break, stratigraphically and paleeontologically, that occurs from the base of the Potsdam to the top of the Lower Helder- berg, and because it approaches nearer the line of division established by Murchison than any other thus far discovered. Wherever the Hudson River Group has been examined upon the continent, the superimposed rocks are unconformable with it, and no passage beds exist. In the western States the Niagara Group succeeds it. In the eastern States it is succeeded by the Medina and Clinton Groups before the Niagara is reached. On the Island of Anticosti, however, where the Hudson River Group has a thickness of 950 feet, it is succeeded by rocks resting conformably upon it, and with no apparent physical gap between them, although there is a sudden paleontological break. Of the 121 species known to Prof. Billings from this group, 80 suddeuly disappear below the break, 41 only passing upward where they are as suddenly joined by 45 species unknown in the Lower Silurian strata. This hiatus or dividing line between the Lower and Upper Silurian will be more distinctly realized when we reflect, that from the Potsdam, out of 62 genera, 46 passed to higher groups, and 20 of these passed beyond this line, and yet, when all the genera from the Lower Silurian are considered, making 280, only 120 passed this line, notwithstanding the latter number came into existence in the Trenton, Utica Slate and Hud- son River Groups, which are so intimately connected, and immediately precede this dividing line. yo 288 Cincinnati Society of Natural History. THE UPPER SILURIAN. The Upper Silurian is subdivided into the Medina Group, Clinton Group, Niagara Group, Onondaga Salt Group, Guelph Group, and Lower Helderberg Group. The Medina Group.—This group includes the Medina sandstone, Oneida conglomerate and Gray sandstone. It was named from Medina, New York. The Medina sandstone was described by Vanuxem, in 1842, and redescribed by Hall, in 1845. It usually consists of red, marly or shaly sandstone, or variegated light-red and yellowish sandstone, and gray quartzose sandstone. In its geographical distribution it extends from New York into Canada, and as far west as Lake Huron, and from New York across Pennsylvania, Maryland, Virginia, and into Tenn- essee. Between the mouth of the Niagara river and Lewiston, it is 300 feet in thickness; at the west end of Lake Ontario, in Canada, 614 feet; on Lake Huron, 103 feet; and in Pennsylvania and Virginia, from 1,000 to 1,500 feet. The Oneida conglomerate was defined, in 1843, by Prof. James Hall, as a quartzose conglomerate succeeding the Hudson River Group in the eastern part of New York, and a gray sandstone in the western part. In 1842, Vanuxem described the gray sandstone, and showed that it is intimately connected with the Medina sandstone. Its thickness in the region of Lake Ontario is less than 100 feet, but it extends south- wardly increasing in thickness in Pennsylvania and Virginia, so that its maximum thickness in the latter States is not less than 700 feet. This thickness is included in the statement above of the thickness of the Medina Group. The character of the conglomerate is such that it indicates rapid deposition, and it is almost non- fossiliferous, though a few fragments of fucoids and shells too im- perfect for definition have been found init. The conglomerate and gray sandstone are included in the Medina Group, because the gray sandstone, in some places, graduates into the Medina so that they can scarcely be distinguished, except by the color, and for the still stronger reason that there are no fossils to characterize it. The accumulation of the deposits, in this group, seems to have been more or less affected by waves and currents, and probably where it has its greatest thickness, took place with some rapidity. The most that can be said of it is, that it indicates a vast and important chasm in geological time. The fossils are usually very poorly preserved. The only genera commencing an existence in this group are Arthro- Observations on the Unification of Geological Nomenclature. 289 phycus, which is peculiar to it; and Dictyophyton, which continues as high as the Chemung. The Clinton Group.—This group was named from the town of Clin- ton, in Oneida county, New York, and was very fully defined by Van- uxem, in 1842. It consists of green and black-blue shale, greenish and gray sandstone, red sandstone often laminated, calcareous sandstone and red fossiliferous iron ore beds. It has an extensive geographical distribution in the region of the Appalachian chain, and thins from it rapidiy westward. In its extension north and south, it reaches from Georgia and Tennessee into Canada, and in its extension east and west, from Newfoundland to the Lake Superior region, though it does not appear in Indiana and Illinois. The thickness in the Lake Superior region is less than 50 feet; at Hamilton, Canada, 136 feet; and in New York, about 400 feet. It increases southerly until it reaches, as is sup- posed, in Pennsylvania, a thickness of 1,600 feet. In Newfoundland, where it is not clearly separable from the Niagara, both together have a thickness of 2,800 feet. In Georgia and Tennessee the thickness is about 400 feet. In some places the Medina so graduates into it that the line of separation is hardly determinable, and at other places it be- comes very intimately blended with the Niagara Group. The distribution of the genera supposed to have commenced an ex- istence in this group is as follows: In the vegetable kingdom, Zchnophycus is peculiar to it. Among the Polypi, Acervularia, Chonophyllum, and Cyathophyllum extend to the Carboniferous; Hridophyllum, Ptychophyllum, Cysti- phyllum, and Strombodes, extend up into the Devonian; Cannopora, and Omphyma, occur in the Niagara Group, and Cyclolites is peculiar to it. Among the Echinodermata, Ichthyocrinus occurs as high as the Burlington Group; Caryocrinus occurs in the Niagara; and Clostero- crinus is peculiar to it. Among the Bryozoa, Rhinopora and Helopora occur in the Niagara. Among the Brachiopoda, Chonetes extends to the Permian; Meris- tella and Pentamerus to the Hamilton; Strophodonta to the Chemung; and Leptocelia to the Upper Helderberg. Among the Cephaiopoda Discosorus and Huronia extend to the Niagara: and Glossoceras is peculiar to it. Among the Lamellibranchiata, Pyrenomeus is peculiar to it. Among the Crustacea, Phacops and Homalonotus extend to the Upper Devonian. 290 Cincinnati Society of Natural History. Of the twenty-seven genera thus enumerated as commencing in this group, five did not pass beyond it, seven became extinct in the Niagara, ten in the Devonian, and five passed up into the Carboniferous. Pentamerus oblongus, Spirifera radiata, Meristella cylindrica, Lingula lamellata, Caryocrinus ornatus, and many other species pass from the Clinton to the Niagara, so that the groups are strongly con- nected specifically, as well as graduating into each other. The Niagara Group.—This group was so named from its develop- ment at Niagara Falls. It was defined by Vanuxem, in 1842, and more fully by Hall, in 1848. It consists of limestones and shales, and sometimes sandstones, though changing its lithological characters and combinations in different and distant localities. It is one of the universal groups. In New York and the southern part of Canada, its thickness is from 250 to 300 feet, on Grand Manitoulin Island, 560 feet; on Cockburn Island, 400 feet; in the Lake Superior region, 300 feet; in Ohio, Indi- ana, Illinois and Iowa, about 600 feet; and in Missouri about 200 feet. Its greatest thickness, however, is in Tennessee or Newfoundland, but the measurements that have been made at these places have left the exact thickness uncertain. 3 It is so well characterized by its fossils, that there is, usually, no difficulty in determining it at any locality, nothwithstanding any change that may have taken place in its petrological characters. The distribution of the genera supposed to have commenced their career in this group, is as follows: Among the plants, Psilophyton extends to the Devonian, and Giyptodendron is peculiar to it. Among the Protista, Astrwospongia extends to the Hamilton; and Aulocopina and Paleomanon are peculiar to it. | Among the Polypi, Amplexus, Cyathaxonia, and Syringopora pass up into the Coal Measures; Striatopora to the Burlington, Antho- phyllum, Blothrophyllum, Cladopora, Diphyphyllum, Limaria, Lyellia, — Thecia, Thecostegites, and Vermipora pass up into the Devonian; Calceola to the Lower Helderberg; Baryphyllum to the Onondaga Salt Group; and Acanthograptus, Astreophyllum, Calophyllum, Calyptograptus, Cenites, Cystostylus, Dictyostroma, Ethmophyllum, Inocaulis, Plasmopora, Rhizograptus, Syringolites, Strephodes, and Vesicularia are peculiar to it. Among the Echinodermata, Cyathocrinus and Potervocrinus ex- tend to the Coal Measures; Actinocrinus to the St. Louis Group; | Observations on the Unification of Geological Nomenclature. 291 _ Platycrinus to the Kaskaskia; Calceocrinus and Melocrinus to the Warsaw; Codaster to the Burlington; Aptocystites, Ampheristocrinus, Callocystites, Coccocrinus, Crinocystites, Cystocrinus, Echinocystites, -Eucalyptocrinus, Glyptaster, Gomphocystites, Hemicosmites, Hetero- cystites, Holocystites, Lampterocrinus, Lyriocrinus, Macrostylocrinus, Myelodactylus, Pisocrinus, Saccocrinus, Spherocystites and Stephano- crinus are peculiar to it. Among the Bryozoa, Polypora extends to the Coal Measures; Cal- lopora to the Keokuk; Hemitrypa and Paleschara to the Lower Helderberg; and Hornera, Lichenalia, Sagenella, and Thamniscus are peculiar to it. Among the Brachiopoda, Spirifera passes to the Jurassic; Athyris to the Coal Measures; Centronella, Cyrtinu and Nucleospira to the Subcarboniferous; Coelospira to the Corniferous; Anastrophia and Rhynchospira to the Lower Helderberg; Monomerella and Trimerella to the,Guelph; and Cyrtia, Meristina and Skenidium are peculiar to it. Among the Gasteropoda, Platystoma extends to the Coal Measures ; Strophostylus to the Upper Helderberg; and Zremanotus is peculiar to it. | Among the Cephalopoda, Streptoceras is peculiar to it. Among the Lamellibranchiata, Goniophora extends to the Chemung; Megalamus to the Guelph; and Amphicelia and Palewocardia are peculiar to it. Among the Crustacea, Cyphaspis is peculiar to it. Of the 90 genera thus supposed to have commenced an existence in this group, 49 never passed beyond it, 8 became extinct in higher groups of the Upper Silurian, 13 became extinct in the Devonian, and 20 passed into the Carboniferous or beyond. This group is remarkable for the abundance of its fossils, and for the appearance of such a large number of new genera, as well as for the exceedingly great proportion that became extinct within it. It is really the only universal group in the Upper Silurian, and, therefore, constitutes the great body of it, for the groups which succeed in this formation are quite local in distribution, in comparison. The Onondaga Salt Grovp.—This group is limited in its geographi- eal distribution, though it occurs in Pennsylvania, and extends from New York into Canada, and thence northwestwardly to Lake Huron, Mackinac, and the Lake Superior region. It was named from Onondaga county, New York, .and was defined by Vanuxem, in 1842, and further defined by Hall,in 1843. It consists, usually, of marls and thin shaly 292 Cincinnati Society of Natural History. limestones containing salt and gypsum. In Wayne county, New York, it has a thickness of 1,000 feet, but about Grand river, in Canada, it is reduced to 300 feet; about Mackinac, to 40 feet; and in the Lake Superior region, to less than 50 feet. It is not very fossiliferous, and only three genera are known to have commenced their existence in it, viz: Hurypterus which passed up as high as the Coal Measures, Pleurodictyum which occurs in the Lower Helderberg, and Zusarcus which is peculiar to it. It was called the ‘Onondaga Formation,” by the Canadian Geologist, in 1863, and it is an improvement to drop the word “salt,” and call it simply the Onondaga Group. The Guelph Group.—The Niagara Group is succeeded in western Canada by a lenticular mass, having a maximum thickness of about 160 feet, which was defined by Sir Wm. Logan, in 1863, as the Guelph Group, from the town of Guelph, where it is well exposed. It is a limestone dolomite, and may have been a brackish water deposit. It is particularly distinguished by the total absence of the remains of the Echinodermata. It contains many species peculiar to it, but is not characterized by the appearance of any new genera. The Lower Helderberg Group.—This group was named from the — Helderberg mountains, in New York, and was defined by Hall, in 1859. It is composed of a series of limestone strata, and has an ex- tensive distribution in the eastern part of the continent. It is 500 feet thick in New York, and extending eastwardly it reaches its greatest dévelopment at Gaspe, Canada, where it is 2,000 feet inthickness, It occurs in Maine and in Pennsylvania, where it is 1,700 feet in thick- ness, and in Tennessee where it is only 100 feet thick. The distribution of the genera, which are supposed to have com- menced an existence in this group, is as follows: Among the plants, Annularia extends to the Coal Measures. Among the Polypi, Spherolites is peculiar to it. Among the Echinodermata, #driocrinus extends to the Upper Helderberg; Aspidocrinus, Brachiocrinus, Coronocrinus, Dictyo- crinus, Mariacrinus, and Spherocystites are peculiar to it. Among the Bryozoa, Ichthyorachis is peculiar to it. Among the Brachiopoda, Katonia, Merista and Rensseleria extend up into the Devonian, and Camarium is peculiar to it. Among the Lamellibranchiata, Mytilarca extends to the Subcar- boniferous; Megambonia and Ilionia to the Upper Helderberg, and Peteronitella is peculiar to it. Observations on the Unification of Geological Nomenclature. 293 Among the Crustacea, Dolichopterus extends to the Coal Measures, and Pterygotus is peculiar to it. Of the twenty genera that commenced an existence in this group, eleven never passed beyond it, three are known in the succeeding group of the Lower Devonian, three became extinct in higher groups of the Devonian, and the other three passed up into the Carboniferous. With this group we close the Upper Silurian, because we have here another great stratigraphical and palzontological break, and because we have arrived, as near as can be determined, at the top of the for- mation as established by Murchison. Out of 141 genera that com- menced an existence in this formation, 82 became extinct within it, or a much larger proportion than became extinct among the genera that arose in the Lower Silurian. The paleontological chasm is, therefore, wider between the Upper Silurian and the Devonian than it is between the Lower and Upper Silurian. In conclusion, it may be proper to remark, that among the genera from these formations there may be a few synonyms, and while numerous species will be added to the 3,560 that have been described, it is not probable that many genera will be added to those mentioned. I am not prepared to draw the comparison between the groups which have been thus established, in North America, and those within the same formations in Europe and other countries, because this must be done after great study of the variable specific characters, and an ex- haustive comparison of the species. If, however, 1 have broken the ice, in this regard, and furnished any assistance to others by calling attention to the distribution of the genera, it is all that can be ex- pected. THE PREHISTORIC MONUMENTS OF ANDERSON TOWNSHIP, HAMILTON COUNTY, OHIO. By Cuartes L. Merz, M.D. Anderson township is situated in the southeastern portion of Ham- ilton county, the Ohio river forming its southern and southwestern, and the Little Miami its northern and western boundaries; at a point near the junction of the two rivers is the village of California. The general surface or plain of the township, is elevated about six hundred feet or more above the Ohio, and broken up by deep ravines, especially on its southern and western borders, Whilst along the course of the Ohio, the 294 Cincinnati Society of Natural History. township presents an almost precipitous front, the slopes bordering the Little Miami are much less abrupt, receding gradually for a half mile to a mile from the stream. A plain of rich alluvial or bottom land varying from one eighth to three quarters of a mile in width, oc- cupies a position bettween the bluffs and the rivers. Jutting out from the hills or bluffs are plateaus, of drift gravel formation, having a range of elevation of from thirty to one hundred feet above the first bottom of the river. On these elevated plains along the course of the Little Miami river, the Prehistoric Monuments are found in greatest number. . In the northeastern portion of the township, located on a level pla- teau, elevated about one hundred feet above the Little Miami river, and in surveys Nos. 1775 and 1575, is an interesting group of earthworks. Of this group several of the most prominent were described in a former paper, entitled the ‘“ Prehistoric Monuments of the Little Miami Val- ley,’* and designated as Group D on the accompanying chart. Since — the time of the publication of the above mentioned paper, many ad- ditional works have been discovered. In the present paper, I shall continue the same enumeration as in the former, and designate this Group D accordingly, so as to avoid confusion. No. 1 of this group is the largest and most important earthwork in this portion ofthe valley. It is located on-an elevated ridge, about four hundred yards west of Mr. Michael Turner’s residence. It consists of a circular embankment, inclosing an area of about four acres. This em- bankment has a gateway to the southeast thirty-six yards wide: leading from this gateway is a causeway one hundred feet wide, and extending three hundred feet. A mound five and a half feet high is located just within the gateway. An interesting description of this work by Col. Chas. Whittlesey, was published in Smithsonian Contributions, Vol. iii., Art. 7, May, 1850;+ and in a paper entitled “ The Antiquities of the Miami Valley,” Cincinnati Chronicle, November, 1839, by T. C. Day, Esq. Col. Whittlesey erroneously located this work in Clermont county, whereas it is situated in Hamilton. No. 2 0n chart is a circular em- bankment, having a diameter of about one hundred and twenty-five yards. The material for its construction was evidently taken from | within the inclosure. The level of the inclosed area being from eighteen to twenty-four inches lower than the general plain on which * Vide This JouRNAL, Vol. i., No. 8, Oct., 1878. + See supplementary plan, by Col. Charles Whittlesey, on chart. the work is located. The work has a gateway about forty feet wide to The Prehistoric Monuments of Anderson Township. 295 the southeast. The embankment has an elevation averaging two feet. The plain immediately west of this circle is the site of an ancient — cemetery, human remains having been found ata depth of two feet; the interments, as far as known tothe writer, being in the horizontal posi- tion. The extent of this cemetery is about two acres. Nos. 3, 4 and 9 ef this group are a chain of mounds ranging from southwest to northeast. They aretwo hundred yards south of work No. 2, and on the same level. The largest of these mounds (No. 3) has an elevation of twelve feet, and a circumference at base of about two hundred and fifty feet. The next, No. 4, has an elevation of five feet, circumference at base one hundred and fifty feet. Mound No. 9 is about three feet ° high, and has a base about the same dimensions as No. 4. Mound No. 5 is located about four hundred feet east of work No. 2, and in a field annually cultivated, it is of very regular shape, and has an eleva- tion of three feet, with a circumference at base of one hundred and fifty feet. Mound No. 10 is situated on the same plain, and three hundred feet east of No 5, elevation five feet, circumference at base one hundred and fifty feet. On the lands of Mr. Gano Martin can be traced two parallel lines of embankment. (Group D, No. 11 on chart) extending E.N.E. for about three quarters of a mile. These parallels are about two hundred feet apart, and where they are protected by the fence lines, are about eighteen inches in height, and from ten to twenty feet in diameter. They formerly, I am told, terminated in a small circle, the site of which is occupied by the residence of Mr. Martin. They evidently had some connection with the interesting work on the lands of Mr. Turner, described by Col. Whittlesey and others previously referred to. The next group— | GROUP C Is located on the first and second plain along the line of the Cincinnati & Eastern Railway, and the line of the Batavia turnpike, on surveys Nos. 427, 500, 65, 32,567 and 624, and in the vicinity of the village of Newtown. No. 1 of this group, a mound, is located on the west bank of Dry run, just north of the Batavia turnpike crossing. Its elevation is about eight feet, diameter at base about eighty feet. Mounds Nos. 2,3 and 4 are located on the second plain of the river, which has here an elevation ranging from forty to sixty feet. Nos. 2 and 3 are about two feet higher respectively, are annually cultivated, and will before long become entirely obliterated from that cause. \ 296 Cincinnati Society of Natural History. Mound No. 4, the largest of the three mounds, has an elevation of ten feet, and at base a circumference of two hundred and fifty feet. “ It is well preserved, and has a beech tree crowing on its eastern slope. These mounds are about two hundred feet apart, and range westwardly. No. 13 of this group is located on the northeastern portion of this plain. It consists of a circular embankment about one hundred feet in diameter. This work is now almost entirely destroyed by the cut made through the edge of this plain for the New Richmond Railroad. Mounds 5 and 6 are situated in a field south of the turnpike, on the same plain as Nos. 2,3 and 4 on the lands of Mr. Abner Hahn, and are respectively five and three feet in height, Mound No. 7 is known as the “big mound;” it is the largest in Hamilton county. A description by T. C. Day, published in the Cin- cinnati Chronicle, August, 1839, entitled “The Mounds or Tumuli of the Little Miami Valley,” is as follows: “About a mile east of Newtown, in this county, on the farm of Levi Martin, is a mound of the largest class. Its shape is an ovak oblong, rounding to its apex with the most perfect accuracy. It is situated on a shelf of land about thirty feet above the alluvial bottom of the Little Miami river. The soil around is gravelly, but the material of its structure, as usual, is a brick-elay. Near its summit is a large beech, probably two feet in diameter, and its sides are covered with a thick growth of underwood, with several large forest trees. It. is within three hundred yards of a high range of hills, and could not, therefore, have been erected as a watch tower or a place of defence. It has never been opened, but the most probable conjecture is, that it is the monument of some mighty chief, who lies interred in its centre. The plain around its base is perfectly ievel, except within two hundred feet of what was probably its original circumference, the washings of the rains have filled up to a considerable height. The dimensions of this mound, from actual admeasurements, are as follows: Cincumferencerat: WAS. 06 ':,.\ae tia anes 5 Se ree 600 feet. Width af paser eh ie i. eos oa er Lames Weneth Of atibaeee tec his a th ola 250 “ Perpendicular Mersin) 23 ose ss dint ee 40“ Covering an area of an acre.” A recent measurement (July, 1878) by the writer, gave the height as thirty nine feet, circumference at base six hundred and twenty-five feet. Col. Chas. Whittlesey, in Vol. lii., Smithsonian Contributions, 7 — Art. 7, May, 1850, describes this mound, and figures it in Plate iii., No. «se [he Prehistoric Monuments of Anderson Township. 207 2. Hehas, however, erroneously described the mound as being located one mile north, instead of one mile east, of Newtown. Three hundred yards west of, and on the same plain as the big mound, is located mound No. 8 of this group. It is three feet in height, and at base has a circumference of one hundred and fifty feet. The asterisk directly north of this mound indicates the site of a mound that was entirely removed during the construction of the Batavia turnpike. Mound No. 9 is located east of the village of Newtown, in the center of the Odd Fellows’ Cemetery, and on the higher portion of the first plain or bottom land. It is very symmetrical in shape, having an elevation of about ten feet, circumference at base two hundred and ten feet. A small mound (No. 14 on chart) three feet in height, is situated on the east side of the same inclosure. An asterisk on the Plainville road, north of the village, marks the site of a mound recently removed. It was about seven feet in elevation. An account, by S. A. Bell, of its removal and contents was published in the Cincinnati Gazette, March 30, 1874, an extract from which is as follows:. “Mr. S. A. Bell, of Plainville, brought to our office, on Saturday, some pieces of wood almost carbonized into charcoal, a number of fragments of bones, evidently those of young children, and fragments of teeth, back and front, which must have belonged to the mouth of a child; and also a rodent animal's tooth, which had obviously. been worn as aveck ornament. They were found Jast week under an ancient mound, which was removed for the purpose of building the approaches to the Newtown bridge. They lay in a large bed of coal and ashes, which already indicated that the fire had covered a space twenty-five feet in diameter. That it must have been a very hot and long con- tinued conflagration, was evident by the hardness and color of the ground and remains which had been effected by the heat. When the fire had burnéd out, the coal and ashes had been raked together in a heap from four to ten inches in depth. From this heap the pieces of | bone in the collection shown to us have been picked out. Among the : discoveries were a skull which had escaped complete combustion, but . had been flattened down by the weight of the dirt above it, leaving its character plain and distinct, however; close beside it lay three front and four jaw teeth, seemingly unaffected by fire. Most of the other bones lay promiscuously among the ashes. The number of victims was evi- dently large, and (the remains) were all those of children.’’ Two hundred yards northwest from the site of the mound just de- 298 Cincinnati Society of Natural History. - scribed, and within a small private burial inclosure is a small mound (No. 15 on chart), it has a diameter of forty feet at base, and an eleva- tion of about three feet. An asterisk near the junction of the two turn- pikes, in Newtown, shows the site of a mound removed previous to 1830; five skeletons were found with their heads toward the center of the mound in a circle. An asterisk in the center of the village marks the site of a mound removed about the same time as the former one just deseribed. Of this mound, Mr. Wm. Edwards, who is one of the oldest residents, and a most intelligent and reliable observer, says: “The hands in the Newtown district were working on the road, when it became necessary to remove a small mound in front of Mr. Dunseth’s house, in Newtown, where they found five skeletons, and a pot, appa- rently formed of mussel shells, and a kind of glutinous cement. It would probably have held a gallon, and was perfectly formed in shape. It was found in the center of the mound, and the skeletons lying reg- ularly around it, with their heads toward it as a common center. Several other mounds have been removed where the skeletons have been placed in the same positions.” Immediately to the south of Newtown is an elevated plateau, about four hundred yards wide, extending to a small stream called Jennie’s run, which flows along its southern base. This plain is elevated about eighty feet above the level on which the village is located. It is of drift gravel formation, and extends westward about a half mile. About the centre of this elevated plain, and on its northern edge, a mound (No. 16, Group C) is located. This mound is truncated, having graded ways extending to the top of the mound, from the north and south — sides. It has an elevation of ten feet, and a diameter from east to west of sixty feet. On the southern edge and slope of this plateau, and in a line with this mound, a great number of skeletons were dis- covered and exhumed in the summer of 1838. Of this discovery, Mr, T. C. Day, an enthusiastic archeologist of that time, ‘writes: “ Last summer, the workmen, in procuring gravel for the Batavia turnpike, © immediately in the rear of Newtown, in the bank of a small stream called Jennie’s run, disinterred an immense number of human skele- tons. This ancient burial ground is on a gravelly point that juts out from the bank into the run, forming an acute bend. The graves are not, on an average, more than two feet in depth, though probably they were a great deal deeper, as the ridge has evidently washed to a con- siderable degree. As far as caved, the point is a solid body of coarse gravel, till within about two and a half feet of the surface, which 3s _ The Prehistoric Monuments of Anderson Township. 299 \ composed of sand and loam. ‘The skeletons lay in the sandy stratum between the gravel and earth, and so far as preservation is concerned, it has answered the purpose well. Whole anatomies have been ex- humed in an excellent state of soundness, the teeth particularly, some of them as white as ivory, and perfect in every respect. Forest trees, such as beech, sugar, and oak, some at least two feet in diameter, were growing immediately over the graves, and their gnarled roots twisted fantastically through the skulls of these remnants of an ancient people. A fall of gravel would frequently leave bare the whole front of a grin- ning skeleton, seemingly thrust in the grave, feet foremost, and in fact the whole of the bodies bore evidence of a promiscuous burial, some placed horizontally, facing the west, others level, anon a group of four heads within a space of two feet, and in every imaginable position. | About twenty feet from the first discovery of the bones, the workmen came to a large body of charcoal, and the remains of a stone fire place. An earthen vessel was found by some boys, which was broken and de- stroyed before an actual description could be obtained. Several of the skulls exhibited traces of violence, such as would lead one to suppose that this had been a scene of carnage, and the dead bodies thus fur- nished a rude and hasty burial.” Mr. Wm. Edwards visited the grounds during the time that the excavations were being made, in company with Mr. Day, the writer of the above extract, and verifies all he says as true; he also further states that there were a large number of bodies exposed during the grading of the road; and since that time curiosity has led a great many people to visit the place and dig for bones. Mr. Day and himself went to the bank and dug out the four skeletons, fire place, and charcoal, as de- scribed above. Mound No. 11 is located on the east side of the road, leading from Newtown to Clough creek, and three quarters of a mile south of the village. It has an elevation of fifteen feet, and a circum- ference at base of two hundred and twenty-five feet. This mound was designated in a former paper* as the Jewett mound. On the same road, and about one half mile further to the south of this mound (No. 11), located on the third plateau or dividing ridge between Jennie’s run and the Clough creek, is an oblong mound (No. 17, Group C) eight feet high and one hundred and twenty-five feet in length from north to south. Four hundred yards northwest from the west end of the village of Newtown, on the lands of Mr. A. Hahn, is the site of an ancient * This JOURNAL, vol. i., p. 125. a” all “SF ey 300 Cincinnati Society of Natural History. village or camp (No. 18, Group C); it occupies the more elevated portion of the first bottom ofthe Little Miami river. Here numerous flints, arrow heads, pipes, fleshers, potsherds, animal remains, together with charcoal and ashes, are turned up by the plow. On the still higher portions of this plain several human skeletons have been discovered interred hori- zontally (No. 19, Group C). During the course of the present month (October, 1881), a small pit was dug immediately west of the house. At the depth of 3 feet a skeleton was found horizontally interred. Two and a half miles northeast of the village, on the Newtown and Milford road, is a tongue of land extending out from the second plain of the river, having an average height of about sixty feet, anda width of from one hundred to three hundred yards, It is located in survey 427, on the lands of Mr. Samuel Edwards, and is the ridge on which the residence is situated. The extreme northern point of this ridge is occupied by an ancient cemetery (No. 20, Group C). It has not been sufficiently explored to determine the position of the inhumations. Two hundred yards south of this cemetery, on the same point of land, are two mounds (Nos. 21 and 22, Group C), the former being four feet high, and having a diameter of 50 feet north and south. No. 22, the larger mound, has an elevation of eight feet, and measures, at base: two hundred and fifty feet in circumference. These mounds are three hundred feet apart in a line east and west, and about three hundred yards north from the residence of Mr. Edwards. Two hundred yards northeast of the residence of Mr. Edwards, and on the same plateau is located a circular embankment inclosing a mound (No. 23, Group C): The work is a perfect circle, except on the southeast, where it is inter- rupted by a gateway about fifty feet wide. ‘The circumference of the work is about seven hundred feet. The mound is of an oblong shape, and three and a half feet high. The embankment is about two feet in elevation, and the material for its construction seems to have been taken trom within the inclosure, forming a slight ditch. Mound No. 24 of this group is located on a spur of land about one hundred and fifty feet above the level of Dry run, about three hundred yards southeast from the Dry run bridge, and south from the Batavia turnpike. It is composed entirely of flat limestones, of various sizes and thicknesses, and covered with about two feet of clayey loam. It is nine feet in elevation, and has a diameter at base from east to west of sixty feet. It has been opened in its center to a depth of five feet; a layer of charcoal and ashes was reached when the work was discon- tinued. The Prehistoric Monuments of Anderson Township. a0F Mound No. 25 is located on the lands of Mr. L. S. Durham, in the southwest corner of survey 1,126. It is three and one half feet high, and 60 feet in diameter at base; being situated on the edge of an ele vated plateau, ii commands an extensive view. On the lands of Mr. M. Lawyer, in survey 624, and about 200 yards northeast from the resi- dence, is an ancient village site (No. 26, Group C) of probably 4 acres. In addition to several fine barbed arrow points found by the writer at the time of his visit to this locality, a circular disk of bone was found, which proved to be made from a human cranium, probably from one of the parietal bones. Sherds of pottery, flint chips, ashes and charcoal, were also noticed. The extent of the village or camp could be readily determined by the area of black rich soil, contrasting with the sur- rounding light clayey loam. GROUP E. Group Eislocated principally in the vicinity of the Turpin homestead, a quarter of a mile east of the Union bridge, and about two miles west of Newtown. Mound No. 1 of this group is situated north of the Batavia turnpike, and immediately in front of the Turpin residence, on the second plain of the Little Miami river. I¢ has an elevation of about ten feet, diameter at base of about fifty feet. This mound has been considerably reduced in size, its shape being at first oblong; subsequently the ends were removed to make it circular. At that time a large stone pipe representing a frog was found, which is now in the collection of Philip Turpin, Esq. The plain west of the house has long been a re€ort for relic hunters; here are found on the surface, pot- sherds, flints, arrow heads, pot-stones, fleshers, axes, disks, pipes, ete. This level evidently was the site of an ancient village or place of industry (No. 2, Group E). Mr. Edwards informs me that at the time of digging the cellar for the Turpin house, fifty skeletons were removed, besides several curiosities, such as stone pipes of various sizes and shapes. One of the pipes had a bird’s wing beautifully carved on both sides. In setting fence posts along the level where the house stands, they came upon human bones very frequently. The interments were generally in horizontal positions. East of the house, and where the barn now stands, was a small mound, which was about three feet high,—an aster- isk on chart marks the site. South of the turnpike, and east of the Clough creek road, located on the top of the dividing ridge between the Little Miami river and the Clough creek, is a mound (No. 3, Group E) three feet high, and OF oy ie ee Ld +. y fi 4 =f a 302 Cincinnatt Society of Natural History. having a diameter at base of sixty feet. The level east of this mound is known to be an ancient cemetery, the interments being as far as noted in the horizontal position, and under flat limestones; west of the Clough road, on the same level numerous flint and stone implements, potsherds, animal remains, and occasionally human remains are furned up by the plow. The soil is here very dark in color for an area of two acres in extent, whilst the surrounding surface is ofa peculiar gravelly reddish loam. Westward from the Union Bridge is a ridge of land, known as the sand ridge, that forms a series of elevated plateaus, as it extends westwardly for about a mile, and reaches an elevation of over six hundred feet above the first plain. Its greatest width is about three hundred yards. After an almost abrupt ascent of about one hundred and twenty-five feet, the second level.or bench is reached, having an area of probably 4 acres. This level is undoubtedly the lo- cation of an ancient cemetery (No. 4, Group E). On the surface, nu- merous potsherds, together with human bones, are found. Many fine relics have been obtained by the writer and others from this locality. Crossing the level another steep ascent of about one hundred feet brings us to the third plain. In the centre of the upper edge of this plain or bench, overlooking the cemetery, was, until recently, a circle of upright stones, ten feet in diameter (No. 5,Group E). These stones were from ten to twelve inches wide, and from four to five feet in length, arranged close together, and forming a circle. From this point the ascent is gradual until the highest point is reached, about » six hundred feet above the Little Miami river. Over this ‘entire slope, broken bowlders, flint chips, fragments of pottemy, arrow flints, stone implements, etc., are found giving evidence of a long and con- tinued occupation. On the lands of Mrs. Williams, on the east side of the Ohio turnpike, surrounded by forest trees, is a mound (No. 6, Group E) eight feet high, with a circumference of two hundred and twenty-five feet at its base. Three hundred yards farther to the south, on the still more elevated lands of Mr. Jacob Betz, located on the east side of the turnpike, and just on the north corporation line of the vill- age of Mt. Washington, is a mound (No. 7, Group E) having-a diame- ter of one hundred feet at base, and an elevation of twelve feet. An ex- tensive view of the Ohio river and Clough creek valleys is obtained from the summit of this mound. East of the village of Mt. Washing- ton, on the road leading from that village to Clough creek, is a mound (No. 8, Group E) located on an elevated ridge overlooking the ‘valley of the creek. This mound is on the lands of Mr. Leiser, and is six feet ‘ The Prehistoric Monuments of Anderson Township. 303 high, and sixty feet indiameter at base. It is one ofa line of mounds extending from the Ohio river to Newtown, and across Hamilton county to the Mill Creek valley, and thence up this valley to Hamilton in Butler county. Through the Clough valley seems to have been the course of a great trail or highway, leading from the Little Miami val- ley to a point on the Ohio river, about where the village of Palestine, in Clermont county, is situated, and along this route many isolated graves, burials under stone heaps, and beds of charred wood and ashes are discovered. On the Henry Brachman estate, near Cedar Point station, on the Cincinnati & Portsmouth R. R., is a mound three and a half feet high, and 40 feet in diameter; it is situated in a field annually cultivated. GROUP F. Is situated principally on the summit of the high hills above the town of California, on the Ohio river, and north of the New Richmond turnpike. No. 1 of this group is a mound located on the second bottom of the Ohio, near the junction of the Ohio and Little Miami rivers, on the lands of Mr. Ebersole. It has an elevation of fully seven feet, and is about two hundred and fifty feet in circumference at base. The level north of the mound, and extending to the Cincinnati and Richmond turnpike, is an ancient cemetery (No. 2, Group ee lei burials are under flat slabs of limestone, and are discovered two feet from the surface. About thirteen skeletons have been unearthed by the plow, but as yet no systematic exploration has been made. In survey No. 397, on the Whetstone estate, located on the summit of a high bluff commanding a most extensive view up and down the Ohio river, is a mound (No. 3, Group F) constructed of flat slabs of imestone of various sizes; the greater portion of the stone visible show _ evidences of the action of fire. It has an elevation of five and one half feet, and a diameter at base of fifty feet. The point on which this mound is situated has an elevation of about six hundred feet above low-water mark of the Ohio river, Directly to the east of this point, and separated from it by a deep ravine, is a cresent-shaped ridge, known as the Hawkins ridge, having an elevation of about six hundred feet above the river. Immediately on the crest of the hill, and overlooking the Ohio river, are five ‘mounds (No. 4, Group F) forming a continuous chain, extending from east to west over two hundred feet. They are five feet high, and have a diameter north and south of about fifty feet. At the time of my visit, 304 Cincinnati Society of Natural History. the mound farthest east had been excavated at its center, and several fragments of a human skeleton, together with a few fragments of burnt limestone were found in the earth thrown out. From the summit of these mounds a view can be had ranging over half of the county, the mounds on Linwood and Norwood heights, respectively, five and seven miles distant, being in plain sight, The point commands the river for miles in both directions. Fifty yards northeast from these mounds, on the same ridge, is located a mound (No. 5, Group F) having an eleva- tion of six feet, and a diameter at base of sixty feet; on its western slope an oak tree five feet in diameter is growing. Two hundred yards northward from this last mound, was located a mound about five and one half feet high, which was removed to make way for the Hawkins’ residence. In the course of the removal of the mound, a skeleton was ° found at its base in a horizontal position, under a layer of charcoal and ashes; the bones showed no indication of the action of fire. In the cranium of this skeleton, a triangular flint arrow point was found im- bedded. The site of the mound is marked on the chart by an asterisk, Northeastward from this ridge, in survey 620, on the lands of Mr. Crotty, located on the crest of a hill, is an oblong shaped mound (No. 6, Group F), having an elevation of eight feet, a diameter of seventy-five feet, and a length of one hundred and twenty-five feet. It commands a view of the Ohio and Little Miami rivers. About four hundred yards northeast from this mound, on the lands of Mr. 8. W. Markley, and about three hundred yards west of his residence, is probably the site of an aui- cient village (No. 7, Group F) covering an area of about two acres. The usual fvcauons such as fragments of pottery, flint, chips, animal a remains, etc., are plowed up. In the northern portion of survey No. 585, y on the lands of J. W. Markley; located on a hill top, is a mound three and — one half feet high, and having a diameter at base of forty feet (No. 7, ee Ee), Contimgins to the eastward until we reach the lands of © . J. Mathews, we find on a level hill top the usual evidence indicat- ing its former continued occupation as a camp or village (No. 8, Group F). GROUP G. This group occupies the southeastern portion of the township. On the lands of the estate of J. A. G. Morton, in survey 1679, on a bluff point just north of the New Richmond turnpike, is an ancient burial place (No. 1, group G). The method of inhumation seems to have been in the horizontal position as far as yet determined. The level LEAS te D4 Mo SECM Mew” aioe BNR Rant ‘ ‘, oe D mY EXPLANATION OF SYMBOLS, \A G Simple Tumulus or Mound. TB Earth-work enclosing Mound \++, Cemetery, method unknown \=, Inhumation at length. \s=, Inhumation in doubled up position &c, [GB Circumvallation Earth-work. 4 Work shop, atelier, place of industry. A. A circle of standing stones. Stone mound. AA Camp or village site. x Site of mound that has been destroyed. yy RW x GROUP D. No. 7 CLERMONT COUNTY, OHIO, Three miles above Newtown. 4 Rich sort A Bottom From Description of Ancient Works in Ohio, B By CHARLES WHITTLESEY, QO — 1850. m() 000 Smithsonian Cont. Vol. II, Article 7. () SCALE 350 Ft. to 1 Inch. \ ‘MOUND / OneMile North of \/ Bottom land. NEWTOWN. Tiron Description of Ancient Works JN OHIO BY CHARLES WHITTLESE XY, S850. CHART OF THE Prehistoric Monuments, —OFr— ANDERSON TOWNSHIP HAMILTON COUNTY, OHIO, =p CHARLES L. METZ, M. D. 1881. SCALE 2 inches to the Mile. a = bengal roreuhaney Pahl yer«| ‘ + la “MBUIGAS How-rlises esl B MOMS reuiih \e yg ,! egelliv 6 gma AA ; biden i eh i bruce enote > The Prehistoric Monuments of Anderson Township. 305 south of the turnpike forming the first terrace of the Ohio river and Five mile creek, shows numerous evidences of its having been formerly occupied by an attelier or village (No. 2, group G). From the ancient cemetery just mentioned, the ridge rises very rapidly and precipitously, until it reaches an elevation fully seven hundred feet above the level of the creek. On the top of this hill, on the lands of J. C. Brill, is located « mound that has an elevation of five feet. It is very symmetrical, and commands a view of over eight miles in all directions. On the lands of Mr. Moses Markley, in survey 608, and located ‘on a hill top, is a mound (No. 4, Group G) four feet high, and forty feet diameter at base. A careful search throughout the territory occupying the central and eastern portions of the town- ship, failed to discover any additional earthworks. Some, however, may possibly have been overlooked. The symbols employed in the accompanying chart, designating the character of the different monuments, are in accordance with the inter- national code of MM. Mortellet and Chantre,* and Smithsonian Cir- cular in reference to American Archeology.t The two supplemental plans, one of the earthworks on the Turner farm (No. 1, Group D), and the other of the great mound east of Newtown, are copied from Plate iii, Art. @ Vol. iii, Smithsonian Contributions by Charles Whittlesey. The earthworks were erroneously located, by that gentleman, in Clermont county, but they are in Hamilton county, as elsewhere stated. The great mound is one mile east of, instead of nortl of, the village of Newtown, and is located near the road leading from Newtown to Batavia, instead of being on the road leading from Newtown to Milford, as stated by Col. Whittlesey. Many of the earth- works in this vicinity are being wantonly destroyed by curiosity-hun- ters who have no other object or desire seemingly than to destroy that which, to the archeologist and ethnologist, is of the greatest im- portance. In conclusion, I would again extend my thanks to Mr. Wm. Edwards, of Newtown, for his very valuable assistance in locating accurately many of the monuments, and for valuable information re- garding them. Acknowledgments are also due to Messrs., William Archer and Charles F. Low, for their valuable assistance in preparing the accompanying chart ; and to Dr. F. W. Langdon for revision of the proof-sheets. MapIisonviL1e, Hamirtton Co., O., October 29, 1881. * Smithsonian Report, 1875. + Smithsonian Miscel. Col., 316, 1878. 306 Cincinnati Society of Natural History. . SUBCARBONIFEROUS FOSSILS FROM THE LAKE VALLEY MINING DISTRICT OF NEW MEXICO, WITH DESCRIPTIONS OF NEW SPECIES. By 8S. A. Mitter, Esq. Prof. E. D. Cope, of Philadelphia, returned from his last annual ex- ploring expedition, in the Western territories, with a collection of in- vertebrate fossils, from the Lake Valley Mining District of New Mexico, which ‘he, very kindly, submitted to the writer for determina- tion and definition. They are from rocks of Subcarboniferous age, and belong to the Burlington or Keokuk Group, but most likely to the former. The following remarks and enumeration of species will — all the light, in our possession, upon the age of the rocks. 1. Strophomena rhomboidalis.—This species, as it is now under- stood, is found in the Trenton, Utica Slate and Hudson River Groups of the Lower Silurian; in the Clinton, Niagara and Lower Helderberg Groups of the Upper Silurian; in the Upper Helderberg, Hamilton and Chemung Groups of the Devonian; and in the Waverley, Burlington and Keokuk Groups of the Subcarboniferous, in America. It is not known to the author higher than the Keokuk. Its Vertical range ex- ceeds that of any other species that occurs in these formations, or in any other rocks of the known world, and its geographical distribution extends to every continent where the strata of these ages have been studied and described. Its form is subject to many variations, and these have received distinct names in different formations, as S. tenwt- striata in the Lower Silurian, 8. depressa in the Upper Silurian, and S. rhomboidalis in the Devonian. And, so far as the author has ob- served, it would appear that the Lower Silurian specimens are usually smaller and have fewer concentric wrinkles over the visceral region than those found in the higher strata of the Upper Silurian and” Devo- nian formations, and that the length of the front and lateral margins, from the geniculation, in the Upper Silurian specimens, is usually greater than it is in Lower Silurian, Devonian or Subcarboniferous specimens ; but these differences are not so constant as to form infex- ible characters, and hence it is that many of the learned and better pale- ontologists have classed them all together under the first and oldest specific name. On the other hand, the similarity between specimens collected in rocks of the same formation in distant countries is re- markable. This is most strikingly illustrated by the fact that a i ti tl ioe gel Ad. r Subcarboniferous Fossils from New Mexico. 307 number of specimens may be selected from the Upper Silurian rocks, in the island of Gottland, in the Baltic sea, and mixed with a like number of specimens from the upper part of the Niagara Group, at Waldron, Indiana, and it will be found extremely difficult for an ex- perienced collector to separate them. 2. Spirifera rockymontana.—This species is represented by a single, small, somewhat distorted specimen, but there is very little doubt about the identification. | 3. Spirifera striata.—This species is found in Bolivia, Ireland, England and Europe, as well as other distant localities, but is rare in the Mississippi valley and. the Appalachian range, It is an everchang- ing species, and yet, throughout all its variations and wide geographi- cal distribution, it is known only in the Subcarboniferous. It occurs in New Mexico in all its forms, from less than an inch to three inches in width, and having a length, in some specimens, equal to the width, and in others but little more than half as great. The hinge line occurs shorter than, equal to, and longer than the greatest width of the valves below. The plications are finer on some speci- mens than on others, and increase in number with the growth of the shell. Throughout all the changes, the ventral valve distinguishes the species by the almost uniform width of the cardinal area, and the gradually widening mesial sinus toward the front, with a corresponding increase in number of the plications, A, Athyris lamellosa.—This species occurs in the Subcarboniferous of Europe, and has been found within the Mississippi valley, and at other places in the West. 6. Athyris planosulcata.—This species occurs in the Subcarbonifer- ous of Europe, and in the Keokuk Group of Iowa and Illinois. 6. Orthis resupinata.—This species occurs associated with Spirifera striata, at various localities in Europe, but is quite rare in America. 7. Orthis michelini.—This is another species of world-wide distribu- tion and great verticalrange. It occurs in the Burlington, as well asin all the other groups of the Subcarboniferous, 8. Productus semireticulatus.—This species, again, is world-wide in its distribution, and is common to the Burlington and Keokuk Groups. 9. Productus vittatus.—This species was described from the Keokuk Group of Iowa. 10. Rhynchonella pustulosa.—This species was described from the Burlington Group of Iowa. 11. Platyceras wquilaterale (misspelled equilatera).—-This species 9 308 Cincinnati Society of Natural History. occurs in the Keokuk of Indiana, Illinois, and Iowa, but is more rapidly expanding than the form from New Mexico. This difference can hardly be of specific importance. 12. Proetus peroccidens._-This species was described from the Sub- carboniferous of the Rocky Mountain region, and though our cae is quite fragmentary it probably belongs to it. 13. Amplexus. fragilis.--This species was described from the Keokuk Group of Iowa, but it also occurs in the Burlington, in the same State, and it is common in the Keokuk of soutbern Kentucky. 14. Cyathophyllum subcespitosum._-This species was described from the Carboniferous of the west, and compared with Cyatho- phyllum pseudo-vermiculare from the Subearboniferous of Ireland, with- out longitudinal sections, The differences between the species are not readily determinable without cut sections, and it is, therefore, a matter of doubt to which species our specimens belong. 15. We have also two undetermined species of Zaphrentis, two unde- termined species of Bryozoa belonging to the family Menestellide, and the fragment of an Orthoceras. It is, however, the appearance of the crinoids, res than the above- mentioned species, that inclines us to refer the rocks to the age of the Burlington, instead of the Keokuk. Brachiopods and corals fre- quently have an extended vertical range, but crinoids are ugually confined to a few feet, and it is an exceedingly rare occurrence for a species to pass from one group to another. The separation of the Burlington from the Keokuk could hardly be maintained were it not for the great change in the character of the crinoids. Of course, in Towa and Missouri, a cherty layer, which Hall, in defining these groups, placed at the base of the Keokuk, separates them; but even here they are so intimately blended, that some authors refer the chert layers to the Upper Burlington. Without any information regarding the appearance of the rocks, in Lake Valley, or whether the fossils are all from the same elevation or not, and looking at the fossils above mentioned, and those hereafter to be mentioned and _ described, and supposing them to come from substantially the same elevation, we would confine the rocks between the base of the Burlington and top of the Keokuk, with the probabilities in favor of the age of the Upper Burlington. There are in this collection three species of Platycrinus, one of them truncated at the hase like P. wortheni, and another having the form of P. planus, though neither species is in condition to be described, and Subcarboniferous Fossils from New Mexico. 30? ¢ one hereinafter defined. With these, there are eight specimens of Actinocrinus, belonging to six different species, two of which are here- inafter described, one cast of a Dorycrinus, and one Dorycrinus which is defined, and also numerous fragments of crinoid columns. ACTINOCRINUS DALYANUS, 0. Sp. Plate VII., fig. 1, view of the azygous side, natural size; fig. la, view of the posterior or side opposite the azygous side of another specimen, natural size. Body below the arms, turbinate, truncate at the base, summit conical and produced into a proboscis. The general form is much like that of A, celatus, though the base is not-so broadly truncated. Basals.—Basal plates twice as wide as high, and thickened at the base. First radials.—First radials about as wide as high, two heptagonal, and three hexagonal, Second radials.—Second radials wider than high, three of which are pentagonal, and two hexagonal. Third radials.—Third radials a little wider Gham high, hexagonal, and supporting upon each of the upper sloping sides a single secondary radial. Secondary radials.—The secondary radials are short, pentagonal, and support upon each of the upper sloping sides a single brachial plate from which the free arms arise. Regular interradials.—Regular Tatornawinls four, the first heptag- onal or octagonal, about the size of the third radials, succeeded by two smaller plates, and these by a single plate resting between the second- ary radials. Azygous interradials.—The first azygous interradial is hexagonal, of about the same size as the first radials. It is succeeded by two plates, and these by three, above which only a single plate appears to occur. : Arms.—Arms twenty. Surface.—The surface is ornamented with a tubercle in the central part of each plate, from which a ridge radiates toward the middle part of each of the sides, uniting at the sutures with like ridges from the adjoining plates, thus forming a stellate and tuberculous decoration. The summit is covered with numerous papilliform, polygonal plates. The specific name is in commemoration of Mr. George Daly, late manager of the Lake Valley silver mines, and a noted mining engineer of superior endowments. He was killed by the Apache Indians. 310 Cincinnati Society of Natural History. ACTINOCRINUS COPEI, Nn. Sp. Plate atta 2, view of the azygous side, natural size ; fig. 2a, view of the opposite or posterior side, natural size; fig. 2b, view of the vault or summit. Body broadly turbinate below the arms, slightly truncate at the base, and depressed convex on the summit. Basal plates about three times as wide as high. First radials wider than high. Second radials wider than high. Third radials wider than high, and supporting upon each of the upper sloping sides a single secondary radial. The secondary radials are short and broad, and support upon the upper sloping sides a single brachial plate from which the free arms arise. Arms twenty. The first regular interradial is about the size of the third radials, it is succeeded by two smaller plates, and these by one or two plates rest- ing between the secondary radials. In the latter respect there is a difference in the interradial spaces. The first azygous interradial is of about the same size as the first radials. It is succeeded by two plates» and these by three, above which there appears to be only a single plate. The plates in the calyx are about the same in number and position as in A. dalyanus, but they are wider in proportion to their height. The summit is covered with numerous conical polygonal plates, with the exception of a large subcentral aperture. Broad shallow depres- sions appear near the margin, which become well defined channels be- tween the arms, especially upon the azygous side. A cast would no doubt show more strongly these depressed interbrachial spaces. The surface of the calyx is very highly ornamented by stellate ridges and sculptured depressions, with verrucose and granulous elevations. It is not surpassed in ornamentation by any species be- longing to the genus. The specific name is in honor of the distinguished naturalist, to whose collection it belongs. : DoRYCRINUS LINEATUS, N. Sp. Plate VILI., fig. 3, view ‘of the azygous side; fig. 3a, view of the posterior or side apposite’ the azygous side, natural size. Body of medium size, turbinate below the arms, truncate at the base, summit depressed, conical, with a prominent subcentral spine. Basal plates twice as wide as high, and extending below the facet for the attachment of the column. First radial plates a little wider than high, three hexagonal, and two heptagonal. Second radials less than half the size of the first, twice as wide as high, and quadrangular 3 Se t } Subcarboniferous Fossils from New Mexico. 311 in outline. Third radials a little wider at the upper lateral angles than the second radials, pentagonal in outline, and supporting upon the upper sloping sides a single pair of smaller secondary radials, each of which supports two brachial plates from which the free arms arise, except as to the right anterior series (the left anterior series is cle- stroyed at this place in our specimen), where three secondary plates appear to rest upon the third radial, and support two brachial plates each, from which free arms arise. A single regular interradial plate fills the space to the top of the secondary radials. It rests between the upper sloping sides of the first radials, and is bounded on either side by the second and third radials, and a secondary radial, and on the top by an interbrachial plate, thus giving it nine sides. Its size is about that of a first radial. The first azygous interradial is longer. than wide, octagonal, and a little larger than the first radials. It supports three interradial plates, the central one of which is followed by an interbrachial plate, which connects with others extending to the opening in the vault, The summit is covered with polygonal, crateriform plates, and a strong subcentral spine approaching the azygous side. The opening is situated below the base of the spine above the level of the arm open- ings, and is surrounded by slightly projecting plates. Supposing the left anterior side to be like the right anterior, in accordance with the usual structure, the species will have twelve arm openings, and if there are two arms to each opening, as is usual in the genus, there will be twenty-four arms. The plates of the body are all more or less tumid. The first radials have an arcuate elevation, and the second radials a tranverse enlargement. ‘The whole surface is marked with fine lines, very con- spicuous under a magnifier, from which the specific name is derived. Those on the body below the arms are longitudinal, but those on the vault seem to radiate from the crateriform depressions in the plates. PLATYCRINUS POCULUM, 0. sp. Plate VII., fig. 4, basal and posterior view, natural size. Body of medium size, sub-hemisvherical or deep saucer-shaped. The three basal plates forma shallow pentagon less than one fourth the height of the cup. The facet for the attachment of the column is subcircular or slightly elliptical and full one-third the diameter of the base. The first radial plates are twice as large as the basals, subquadrangular, a little wider than high, and gradually increase in width from below up- 312 Cincinnatt Society of Natural History. ward. The facet for the reception of the second radial forms a semi- circular depression in the middle of the upper part, and occupies about one half of the summit and extends down more than one third the length of the plates. Sutures, except between the basals, are im- pressed or distinctly channeled, and the surface is covered with well- defined nodes. ‘I'wo rows on the pentagonal base surround the colum- nar facet, and two rows occur on the first radials below the semicircu- lar facet for the second radial. This species is founded upon a single specimen, showing only the parts above described. It has some weight, in connection with the other species of crinoids, as evidence, in determining the age of the rocks, and can, no doubt, be readily identified, imperfect as the type specimen may be. TREMATOPORA AMERICANA, D. Sp. ' Plate VII., fig. 5, fragment natural size; fig. 5a, magnified view. This species consists of irregularly cylindrical, ramose, hollow stems or branches. The interior is evidently lined with an epitheca. The diameter ofthe stems examined is from two tenths to six tenths of an inch, and the thickness of the corallum is from less than half a line toaline. The thickening of the corallum is not dependent upon the size of the branches, but seems to be the result of irregular growth. The cell tubes are subcircular and irregularly distributed. The aper- tures are margined by a projecting lip which sometimes overshadows the lower part of the opening. There are usually about four cell tubes in one tenth of an inch where the intervening spaces are about one and a half times the diameter of the tubes, but owing to the scattered distribution of the tubes, the proportion is variable. There is neither uniformity in the shape of the branches, nor in the order of a _ahge- ment of the cells. TREMATODISCUS ROCKYMONTANUS, 0. Sp. Plate VII., fig. 6, view, natural size. Sheil medium size, discoidal; umbilicus wide, showing the inner whorls and perforated in the middle; volutions very gradually increas- ing in size, narrower transversely than from the dorsal to the ventral side, and slightly embracing; septa slightly arching forward on the periphery, and surface ornamented by fine revolving lines. Siphuncle and body chamber unknown. It is supposed that about one whorl has been broken from the specimen described and illustrated. Subcarboniferous Fossils from New Mexico. 313 CAMAROPHORIA OCCIDENTALIS, Nn. Sp. Plate VII., fig. 7, dorsal view ; 7a, ventral side; 7, front view. Shell of variable size, some in the collection having less than one fourth the dimensions of the specimen illustrated. General form sub- trigonal, wider than long, truncated in front, straight upon the postero- lateral slopes and rounded to the front. Dorsal valve gibbous, most convex anteriorly. The posterior lateral slopes are abrupt, the anterior lateral slopes and the front are more or less sharply geniculated, and extend down, meeting the ventral valve near the middle of the front face, but forming almost the entire anterior lateral sides before joining the opposite valve. Mesial elevation flattened anteriorly, but well defined to the middle where it is no longer traceable; a sinus arises anteriorly in the middle of the mesial elevation, and becoming well defined ex- tends to the beak which is incurved beneath the beak of the ventral valve. There are from seven to nine angular plications on the mesial elevation, and about the same on either side, making from 21 to 27 plications, on the specimens examined. Ventral valve somewhat flat- tened, most convex in the central part, from which it slopes in all di- rections, but flattens out or curves up alittle, at the antero-lateral sides, where it is very sharply. geniculated, and unites with the opposite valve; toward the front the curvature increases, terminating in an abrupt geniculation and extension to meet the other valve in the middle of the truncated front. The beak is pointed and eurved over upon that of the dorsal valve. The mesial sinus is broad and defined only on the anterior half of the valve. The plications are the same in num- ber as those that occur on the dorsal valve. The surface of both valves is ornamented by fine concentric lamellee of growth, which, in crossing the angular plications, make a series of zigzag lines, that also ornament the truncated front to the point of union of the serrated valves. This is a handsome species readily dis- tinguished from all hitherto described. ‘ ORTHIS DALYANA, 0. Sp. Plate VIL., fig. 8, ventral view ; fig. 8a, dorsal view ; fig. 8b, profile view. Shell depressed, suboval in outlite, and length about equal to the greatest width, which is at the anterior third. Dorsal valve most con- vex above the middle, from which it inclines in all directions to the margin, forming a broad, flattened inclination toward the front. Beak 314 Cincinnati Society of Natural History. small, pointed and extending beyond the cardinal area. Ventral valve most convex near the beak, sloping off wedge-shaped toward the front, and very rapidly, at first, toward the posterio-lateral sides, but flatten- ing out before reaching the margins. The beak is elevated, sharp, slightly incurved, and extends beyond the beak of the opposite valve. The length of the linear area is about half the width of the shell. The surface is ornamented by numerous fine, round, radiating strie, which increase by implantation, and are crossed by several strong, concentric, imbricating lines of growth, and intermediate finer concen- tric lines. This species, in its surface markings, resembles O. vanuxemi from the Devonian, but the striz are finer and more numerous, and it . may readily be distinguished from other species found in rocks of its own age. SPIRIFERA TEMERARIA, 0. Sp. Plate VII., fig. 9, ventral view ; fig. 9a, dorsal view: fig. 9b, front view. Shell small, transversely subelliptical, moderately gibbous, hinge line less than the width of the shell, and cardinal extremities rounded. Dorsal valve convex from back to front ; mesial fold convex, much elevated at the front, while at the anterior sides of the mesial fold, the shell is rapidly curved down, and produced to meet the truncated ex- tension of the opposite valve on each side of the sinas ; the beak is of moderate size, and arched over the linear area. Ventral valve, gib- bous in the umbonal region, and sloping to the front and sides ; the sinus, commencing with a shallow, rounded depression in the umbonal region, becomes more and more strongly defined, and terminates in a deep, somewhat angular, and much produced extension in front. The beak extends beyond the beak of the opposite valve, and is incurved over the area, which is almost linear. The surface is ornamented with very fine Sue lines, which are crossed by numerous fine concentric lines, and a few stronger imbri- cating lines ofgrowth. There is only asingle specimen of this species in the collection, and it is therefore supposed to be a rare form—hence the specific name. SPIRIFERA NOVAMEXICANA, 0. Sp. Plate VII., fig. 10, ventral view; fig. 10a, dorsal and cardinal view ; fig, 100, front view. Shell more or less gibbous, transverse, triangular, and having the cardinal angles extended into mucronate points. The dorsal valve is ad Subcarboniferous Fossils from New Mexico. | 315 convex from the cardinal line to the front with the greatest convexity in the middle. ‘The mesial fold is round and truncated by the exten- sion of the sinus in the opposite valve. The beak is scarcely defined, and does not project beyond the narrow area which extends the whole width of the shell. Ventral valve more gibbous than the dorsal valve, and most convex at the posterior third. The mesial sinus is rounded, and gradually widens from the beak to the front where it is produced so as to truncate the mesial elevation of the opposite valve. The um- bo is prominent, and the beak sharp and incurved over the fissure. The area extends to the cardinal angles, ts slightly concave, especially in the middle part, and is transversely striated. The surface on either side of the mesial fold and sinus is marked by about six simple rounded plications, which become less prominent as they recede from the fold and sinus. The entire surface is covered by fine, concentric, imbricating lamellose lines, which become more marked toward the front of the shell. RHYNCHONELLA TUTA, nN. Sp. Plate VII., fig. 11, ventral view; fig. lla, dorsal view; fig. 11b, front view; all natural size. Shell small, suboval, greatest width at the anterior third, length and width sub-equal, ventral side most convex. Ventral valve, gibbous, highly convex in the central region; mesial _ sinus, not clearly defined; beak acute and closely incurved upon the beak of the opposite valve. Dorsal valve, moderately convex; mesial depression, imperfectly de- fined; beak acute and incurved beneath the beak of the opposite valve. Surface marked by about eighteen fine, sharply angular, simple pli- cations on each valve. This species is founded upon four specimens, each of which is more or less injured. The lateral and front margins appear to be in one plane. There is uo species in rocks of the same age with which it is necessary to make any comparison. 316 Cincinnati Society of Natural History. DESCRIPTION OF NEW SPECIES OF FOSSILS FROM THE HUDSON RIVER GROUP, AND REMARKS UPON OTHERS. By S. A. Miuuer, Esq. DENDROCRINUS ERRATICUS, 0. Sp. Plate VIII., fig. 1, view of the azygous side, natural size ; fig. Ja, posterior or opposite view. Body obconoidal, rounded at the base, a little longer than the greatest diameter at the top of the first radials, plates smooth, sutures well marked, and more or less channeled above the basals, with de- pressions at the angles. Basals forming a little cup about halfas high as wide, plates pentagon- al, the upper sloping sides shorter than the lateral sides. Subradials regularly hexagonal, much larger than the basals, and nearly as wide as long. Three of the first radials pentagonal, length and width sub- equal, size about equal to the subradials; one on the left side hexag- onal, and larger than the other first radials; the first and second plates in the left anterior series, a little smaller than the first radials, the lower one pentagonal, and the upper hexagonal. The superior side of these plates is equal to the greatest width. The succeeding plates in the first radial series are as wide as the first radials, and have a length about equal to one third the width. A division takes place on the third plate above the first radial in each of the anterior rays, and on the fourth plate in the left lateral ray. Only three or four plates, in each of the arms, are preserved above this division, in our specimen. The first azygous plate is hexagonal, and a little larger than the subradials. The second is hexagonal, and smaller than the subradials. It supports upon its upper side two series of plates, the one on the right composed of very small plates, and the succeeding plate in the left series bears upon its left side a series of minute plates that inter- vene between it and the left anterior ray, so that, at this part of the azygous side, we have a width of three plates, but the marginal rows are very small. In our specimen we have preserved, in the azygous in- terradial area, seventeen plates, six of the larger ones form the central series, four minute plates intervene between this series and the right anterior free arm, and seven between it and the left anterior free arm. The column, as indicated by the columnar facet, is very small. This species bears some resemblance to D. latibrachiatus, from the Hudson River Group, in the Island of Anticosta, and yet it is so distinct as not to require any comparison. ‘ g 4A - ie New Species of Fossils from the Hudson River Group. BEY The specimen described, was found near Cincinnati, where it had evidently been drifted, and is supposed to be from the upper part of the Hudson River Group, possibly from Hamilton or Warren county. It now belongs to the author’s collection. INTERNAL STRUCTURE OF LICHENOCRINUS. Plate VIII., fig. 2, erect, internal lamelle of Lichenocrinus, natural size ; fig. 2a, magnified view. In 1874, the writer described the internal structure of Lichenocrinus tuberculatus, as follows: “Interior filled with upright lamelliform plates, radiating from a central point, on which the exterior plates ap- pear to repose’ (Cin. Quar. Jour. Sci., vol. i., p. 346). No single specimen suitable for illustrating this fact was then known. Recently, I received from Dr. D. T. D. Dyche, of Lebanon, O., a specimen preserving the upright lamellse, and having all the exterior plates removed. The lamelle bifurcate so that the intervening spaces do not exceed the thickness of the lamelle at-.the circumference. The bifurcations do not take place opposite each other in adjoining lamelle, but at different distances from the center, so that uniformity is preserved in the width of the inter lamellar spaces. The divisions take place within the cen- tral depression for the columnar attachment, on the convex circular elevation, and near the circumference. Dr. Dyche’s specimen is from the upper part of the Hudson River Group, within the range of ZL. tuberculatus, and therefore, probably, belongs to that species, though it might, of course, belong toa distinct species as this structure is characteristic of the genus. CUNEAMYA ELLIPTICA, Nh. Sp. Plate VIII., fig. 3, view of the left side of a cast, natural size; fiz. 3a, view of the right side of a smaller cast. Shell very inequilateral, subelliptical, about one half longer than high, greatest height posterior to the beaks, ventricose, and broadly in- flated in the umbonal region; anterior end projecting and rounding from the lunule to the base, which forms nearly a semi-elliptical curve; hinge line, slightly arching; posterior end somewhat truncated in the upper part, and narrowly rounded in the posterior basal region: beaks, prominent, incurved; posterior umbonal region very prominent, and rounded to the posterior third of the shell, and then sloping to the posterior basal region; anterior umbonal region forming a convex elevation extending from the beak to the base, and directed a little backward. « a@ “SNIgidyOH SNsun ate SLOT i Natural 2 9 ES SRY 5 nSorNateral 1 ‘ mimral of the c—/ {| = Jie Vol. «k Cah. nae i Ae Eat ns SACCOCRINUS MARCOUANUS, W. & M.—View of the azygous side of a peculiar specimen, a little distorted and broken off at the con- striction below the vault, natural size, . View of the cast of a vault of another specimen. . SACCOCRINUS URNIFORMIS, n. sp.—View of the left side of a speci- men, natural size, . View of the vault of a specimen which has been a little compressed. . SACCOCRINUS NECIS, W. & M.—View of the azygous side of a medium sized specimen, . . View of the vault of a slightly compressed specimen. . SACCOCRINUS EGANI, n. sp.—View of the left side of a specimen with the piates preserved, natural size. The artist, in drawing, held the base a little too high, at the expense ofa view of the arm openings, though the illustration is correct as seen from the position in which it was taken, . View of the cast of a vault. . ICHTHYOCRINUS CORBIS, W. & M.—View of the anterior side of a specimen having the plates preserved to the commencement of the tertiary series, natural size, : : . 5 5 : XENOCRINUS PENICILLUS, S. A. Miller.—View of the azygous side, showing fourteen plates of the vertical series. The same speci- men referred to on page 73 as belonging to Dr. D. T. D. Dyche, of Lebanon, Ohio, : : , , , ; PAGE. 167 172 175 176 PL A Tea. Figs. 1, la, 16. AGARICOCRINUS CRASSUS.—Prof. Wetherby’s collection, Figs. 2, 2a. NEW CYSTIDEAN.—Prof. Wetherby’s collection, . : ‘ Fig. 3. AMYGDALOCYSTITES HUNTINGTONI.—Mr. Huntington’s collection, Figs. 4, 4a, 4b. AGARICOCRINUS ELEGANS.—Prof. Wetherby’s collection, UD plate a3 t s ——— \ i av PLATE Vi. PAGE. Fig. 1. TRIGONIA STIEBELI, n. sp.—View of the left valve, natural size, . 2259 la. Cardinal view. The right valve of the specimen is unnaturally inflated. Fig. 2. SACCOCRINUS INFELIX, W. and M.—View of the left side of the cast of a moderately large specimen showing the strongly pentangular character observed in some specimens, . : ee 3 - 260 2a. View of the cast of a vault of a small specimen. | 2b. View of the upper part of the cup when the plates are preserved. Fig. 3. CYATHOCRINUS VANHORNEI, n. sp.—View of the left side, natural size. The iower part of the basal plates on the posterior side has been broken off, : . u Fig. 4. GLYPTASTER EGANI, n. sp.—Side view, natural size, 4a. Same magnified. 4b. Basal view. Fig. 5. LEPERDITIA CHCIGENA, n. sp.—Left valve, magnified five diameters, . 5a. Right valve, magnified five diameters. These views may not be pre- cisely accurate because the artist did hot have a photograph to work from. Rico Se Stags fy itan2 Aliny Mery gather, De Journal of the Con Sarde ’ i: S a Dis rald PLATE Vit. Fig. 1. ACTINOCRINUS DALYANUS, n. sp.—Azygous side, natural size. la. Posterior view of another specimen. Fig. 2. ACTINOCRINUS COPET, n. sp.—Azygous side, natural size. e 2a. Posterior side. ; ak 2b. View of the vault. . e - Fig. 3. DORYCRINUS LINEATUS, n. sp.—Azygous side. a 3a. Posterior view. > Fig. 4. PLATYCRINUS POCULUM, n. sp. ss“ Fig. 5. TREMATOPORA AMERICANA, n. sp.—Fragment, natural size. Bs ea Magnified view of part of the same specimen. _ ie Fig. 6. TREMATODISCUS ROCKYMONTANUS, n. sp.—Natural size. ‘Fig. 7. CAMAROPHORIA OCCIDENTALIS, n. sp.—Dorsal view. ane _ ia. Ventral side. Bot 7b. Front view. | : ee: _ Fig. 8. ORTHIS DALYANA, n. sp.—Ventral view. ‘ Bo Pa Oc. Dorsal view. Beet? 8b. Profile view. 8 Fig. 9. SPIRIFERA TEMERARIA, n. sp.—Ventral view. : a 9a. Dorsal view. Dt! 9b. Front view. B ‘Fig. 10. SPIRIFERA NOVAMEXICANA, n. sp.—Ventral view. 10a. Dorsal and cardinal view. 106. Front view. > Fig. 11. RHYNCHONELLA TUTA, n. sp.—Ventral view. 11a. Dorsal view. } 110. Front view—all natural size. ' ee yee ig ote PINE ete WEG OAR Oe 5 o A Ss tah” Me ans ate a ee 3 hearse 5 aa pit Agep as) tS a: aS ; aught fae eee Re eat y; a sr SJ Ay £45 s A ‘ : Bee ae *% > 7 si ae Oe Fo ity aa an te aa ay aie et ib rf ye | vk , we / ‘ Bae “ 6 / st r, Ag a ee 7 py ho ae gs PILATE. VItti. ao & } 2% : tugs Reve. Fig. 1. DENDROCRINUS ERRATICUS, n. sp.—Azygous side, natural size. lu. Posterior or opposite side. oh _ Fig. 2. INTERIOR STRUCTURE OF LICHENOCRINUS—Supposed to be Z. tubereulatus, (eae Fig. 3. CUNEAMYA ELLIPTICA, n. sp.—Left side of a cast, natural size. av 3a. Right side of a smaller specimen. -. Fig. 4. PYANOMYA GIBBOSA, n. sp.—Left side, natural size. Rye cc 4a. Right side. 4b. Cardinal view. : # Fig. 5. ORTHOCERAS CINCINNATENSE. 2s 5a. Specimen slightly worn down. >... Figs. 6.and 6a. ORTHOCERAS HARPERI. are ol - : ase n Figs. 7 and 7a. ORTHOCERAS FOSTERI. = y or Meat Fig. 8. ORTHOCERAS BYRNESI. \ lane » us ¥ s J . : : 4 t i « ¥ i \ is s; oe ~Plate.8 . . AY ‘ pais ’ OF THE 4 } ae , Diet eS etea ; iG ve 2 Hnaingsy BF cee bal Die , * - - % i & : et ites i eh LUA) anya i A NA Pe \ \ Ce, ep Pan ae Hi a} Saal BY Fe d , TEAM UN , } ' i : ¥ poo PU. y ° s pote dz Dn hee atte ee canoe vee n0W,, 0 oy BLISHING COMMITTEE : a) eit ero gees GEO, W, HARPER, » | LAY); 269 VINE STREED. aes of the: ee Veale some Noe and. R markable Crinoids eh Hudson River Group, : 1 _ensis, ae 5 JA. ee ol it i { rvnl rete n Va PNR . y We PUBLISHING COMMITTEE: — ia 4269 VINE STREET." { \ ay” SANE & d Notes on Loui -Fresh-Water Mo cies ‘of Fossils and | Group of Illinois, escriptions of New - boniferons Rocks of Ke The Américan Association fc 4 / . ay AUR N ALS A ah ie cee aad : OF THE o2 pe { j ys : ee Ia es PUBLISHING COMMITTEE: 2 6A) MELLER’. 4 0 BOW. LANGDON. PCB LOW. oo. IF SUDGE,- GEO. W. HARPER. j rect PT abe ea Mae be Wy, Sy f e i Ry Su, OCTOBER, 1881. i) vi yr . MAR 17 1884, Yn, Sy Altec ag _ Proceedings of the Society, .. ; se i Pe: FA Seg t Ses ers ' Mesozoic and Cenozoic Geology. Ganplvaed le Dri Hl Ne e ae . (cio Pant of the Continent, by S. ro ‘Miller, Esq. | The. Century. Plant, by Joseph By “James Seta Us ats The Madisonville Pre-Historie Cemetery ; “Anthropo i a Not co os a a “Description of a ee ‘Species of Patala, and remarks 2 B Description of New Species of | Fossils, * i nate bea ee ee Ht 9 3 em > ee Sa a eae Ue Sloe Fangs F, y s: ve ‘ y, de ni 2 7h rag ; { 3 ! ay fee , Cee j te : Va 4. Dek "Terms: $2 00. ‘per volume ; single number, 60 eer ; 4 a f t 4 ap ‘ ? te PEG) o" , : i ee a t fe Pe es toy re EY : Vat , } ( =, a é 0 pee “ é Wal 4 > é Ae I eg i “ty £ 7 , is 3 y i , / : % eae Pee eects 5 r ? x Hee Fle RY 2 « : tS ye ee 4 EIR Gut. Bhai Bier 5) o earl wa h JOURNAL 2 CINCINNATI SOUIETY OP NATURAL HISTOR ‘ | PUBLISHING COMMITTEE; 6A MIDLER, F, W. LANGDON, eS C.F. LOW, oo ad Bs JOD Gh GEO. W. HARPER. Tee MBER, 1881. A Sn ere me ae Se ne ; er \ 2 & < ie MAR 1 a sae: Or : ‘CINCINNATI: 4 ‘PRINTED BY JAMES BARCLAY, 269 VINE STREET. 3 KX x 3 A ua pF Se ccs. Sp foe} ee é ee Rik Oe iach ee aot LP Aaa Le ee . ss at S : it) rie re = ; Se tater x Bee = — ei, bp es eke < F Med 7S 7 i “x : pA ‘ WM it - ai ry 2 ip J x - ‘ oe) % i : - iat = as - “7 s 0, a 3 : ee Ms ‘ ~ Re aeons y =? 3 3 2 Pa me ay ~~ s); = es es A ts ‘. — a —— ; cS € re me = . sae ZR ~ Sieg A > ; ‘ * : 3 N St ae : % a = CONTENTS Seay : ae — Proceedings of the Soaibey ates ees Sa ae ee eae eee S. ; , j AU ay - ‘ é Observations on the Unification - of Geological ‘Nomenclature, with | j Special Reference to the Silurian Formation of. Ne ae oa “by 8 . A. Miller, D1 Rey flere ee ei Pere ears tat The Prehistoric Monuments of Anderson Township, Hamilton County, Ohio, by Charles. L. Metz, M. Dick Poe ree -Subecarboniferous Fossils from the: Lake Valley Mining District. of \ He, - New Mexico, with Descriptions of New Species, By a AL ye Pi Miller, UT Sas aN NE gO oe er ee se 6 Description of New species ‘of Fossils ees the Hudson River Group, Z : a - and Remarks upon Others, by 8 ok. Miller, Esq. Sie eee Some Notes on American Land Shells, No. I., by A. G. Wetherby, A. M. 323 Zoological ‘Miscellany, by Dr. F. .W. Langdon hoe aie poe ier, -Members of the Cincinnati poctety of Natural History. = ee ae Additions t to ae pe gry 2 = ae single number, 60 cents, wi ——e ~ « 7 ses . 2 | ‘ ) ef i rc ET om xe be \ 5 a date = 7 S Arid u os wy - ~~ F = 7 are es ‘5 ‘ = \ ite / im ee f ts Re ake, " ‘ } avs e x a E 9 =~ 6 je f 2) “+ “ Mee 3 4 Gee ae AIA LES o " se = x re f - Fe. a 4 ~ oe f Ay . — . * Cad AEIEIETEE U3 # ATE AE 2 # GARY OG OWES ef ee ' : = ee He i - . : . : , \ } . \ \ ' t . ‘ ‘ i . 1 ) a : (es ; : - ! ns 2 = 3% 7 > ar 7 A: = + - - nef \. aera ar PET a “So "Fee, ites Sa, po i A | | Eby, bi es a HF Lies eae af eee gr OR ne