Mig x ra ———— - — a ee ae = ioe < HM $ 2 a as e 4 1 ax . Se: ’ * - = e 5 a é 7 oR, . ae” a ee! ae. a ee ea nea im 4 = } ai = > $ : = fe #: PETAR GaP baa UNIVERSITY OF ILLINOIS LIBRARY BOOK CLASS VOLUME eee te a yaa Se Return this book on or before the Latest Date stamped below. XT ARV LIRDARPYV Lepage] ASS p ¢ LIBRAR I | L161—H41 Digitized by the Internet Archive in 2010 with funding from University of Illinois Urbana-Champaign http://www.archive.org/details/panamericangeolo311903desm ha ay CORPS. pp C y i. falar oe ELE PMO AN GEOLOGIST A MONTHLY JOURNAL OF GEOLOGY AND ALLIED SCIENCKS. Editor: N. H. WINCHELL, Minneapolis, Minn. ASSOCIATE EDITORS: FLORENCE Bascom, Bryn Mawr, Pa. CHARLES E. BEECHER. New Haven, Conn. SAMUEL CALVIN, Iowa City, Iowa. JoHN M. CLARKE, Albany, N. Y. ULYSSES S. GRANT, Evanston, Ill. HERMAN L. FatrRCHILD, Rochester,N. Y. OLIVER PERRY Hay, New York,N. Y. PERS!IFOR FRAZER, Philadelphia, Pa. GEORGée P. MERRILL, Washington,D.C. WARREN UPHAM, St. Paul, Minn. ISRAEL C. WHITE, Morgantown, W. Va. HORACE V. WINCHELL, Butte, Mont. VOLUME XXXI JANUARY TO JUNE, 1903 MINNEAPOLIS, MINN. THE GEOLOGICAL PUBLISHING Co. 1903 THE UNIVERSITY PRESS OF MINNESOTA, CONTENTS. JANUARY NUMBER. SKETCH OF THE Lire AND WorK OF THE LATE A. R. C. SELwyn, C.M.G., LL.D., F.R.S, F.G.S., etc., Director of the Geologica! Survey of Canada from 186g to 1894. [Portrait.] H. M. Ami, On RuHOMBOPORA LEPIDODENDROIDES. Meek. [Plate Il.] G. E. COR GHAGS top ook BR OBE Oe OTE EE ERO OC TROL are RET eer VaLitEY Logss AND THE Fosstt MAN oF ene Kansas. War- ren Upham. . PRIA eT tL ae ahs XA ahs 6 ld Sao) tear in, 3 NOETLING ON THE i eee OF THE PeiEcy pops. [Plate III.] IRS IRIAN ETC ae RATA OER BOT Oe, ECE TRE, PSE oo Ee Note on tHe West INDIAN ERUPTIONS OF 1902. G. C. Curtis.... MINERALS OBSERVED ON Buriep CHINESE COINS OF THE SEVENTH ie MRI VA Po leet ICO CRG eh ees Sve GE: de eww het tase bieyeee s AN ERRATIC BOWLDER FROM THE CoAL MEASURES OF TENNESSEE, Pe eR CCE me Nee Uae tye ak oie alia Mae aon RNIN tronic at GEOLOGICAL AGE OF THE West INDIAN VOLCANIC FORMATIONS. J. EPA: SHANTI SA Fe, SE See TM oe Ena ts ACR en een EpirortaL CoMMENT. ie ramondaniness ob Sotth Attica scnsss seis wis saelolecns s Review or ReEcENT GEOLOGICAL LITERATURE. Om Sularpsbackens Dalgang. J. C. Moberg.... Rr Contributions to the Petrography of the John Day fase. Fink Co. MGUY DDS As RO A REIS Oe CRA R Piet ras Oho ee ER one Maryland Geological Survey, vol. IV. W. B. Clark........ Les Roches volcaniaues de la Martinique. A. Lacroix........ MontHiy AutTHor’s CATALOGUE OF AMERICAN GEOLOGICAL LiITER- NAT USRUDY: Ges aA he taca GN eee ee AR ad tT et 8 SL | ee a ea CORRESPONDENCE. Apatite crystals, Antwerp, New York. Nicholas Knight...... Fall Excursions of the Geological Department, Columbia Uni- MCAT APY ec SILLIMET IN. od ina ieee eiog Ue 6 PERSONAL AND ScIENTIFIC News. Chicago Academy of Sciences, 64; Geological Society of Washington, 64; Bath Furnace Meteorite, 64 J. W. Spencer, 65; Am. Inst. Min. Engineers, 65; New Mexico Academy of Sciences, 65; The late meetings of the Geological Society and of the American Association for the Advancement of Science PARRA MRI RO TI ae AOU NG pies rhs Sie soim ois teva sty.t.s 6 vid cede vee oa ne 66272 66 IV Clontents. FEBRUARY NUMBER. GEOLOGY OF THE JEMEZ-ALBUQUERQUE Recion, New Mexico. 4. B: Reagan..*;' [| Plates Ve aerate tester: so. sage > + c\s ree ce Morse on Livinc Bracuiopops. Charles Schuchert.............. TIMBER LANES). (GP Riussellee eae cele. ie oe oie ers) eae Review or Recent GEOLOGICAL LITERATURE. Report of the State Geologist on the mineral industries and geology of certain areas of Vermont. Geo. H. Perkins...... Magnetic declination tables and isogonic charts for 1902, and principal facts relating to the earth’s magnetism. L. A. Bauer, Iowa Geological Survey, Vol. XII, 1901, with accompanying papers. S.' CalvimsanidAenG BL Conare. ii o:ic.. 4 tien ere A system of glacier-lakes in the Cleveland Hills. Percy Fry Rendall 2.2 5 Re erie ae id She alee ree Monruty AutTHor’s CATALOGUE OF AMERICAN GEOLOGICAL LITER- ATURE? 0. ee eee tir) 8 hate ae eae an ee ea PERSONAL AND SCIENTIFIC NEWS. .....---. Geological Society of Washington, 128; Medal awards by the Geological Society of London, 129; Wisconsin Academy of Science, Arts and Letters, 129; Encouragement of mining in the- new Mexican Stole ne Nim esr ae cee me ek nti ener MARCH NUMBER. Tur L H. Harris CoLLtection oF INVERTEBRATE FOSSILS IN THE Unireo States Nationat Museum. [Portrait.] Charles Schucherk: 20 SS ene en ee Brock Mountains 1N Mexico. [Plate XII.] Douglas Wilson EGY Cok ee RIE 2 tes AROSE eas ea eLd ora eine tdicla Sd cic Some EvipENce or Two GLActAL STAGES IN THE KLAMATH Moun- TAINS IN “CALIFORNIA. Oseay lll. Hershey. “coxa. 1. see A Newry-Founp Mererorrre rrom Mount VERNON, CHRISTIAN CouNtY,. .KENTUCKY, (Geo. HP) erin eter. anne Tue Mart-Lorss or tHE Lower WapasH VALLEY. M. L. Fuller Pha a len) coe Coan 1071) eee RIE ero Pert oS ocd lod 4 AG ee. at eC Ames Knos, Norra Haven, Marne; a SEAsmeE Note. Bailey WS Renee he Oe ae Ae ee eee Pe eee On tHE Manttus Formation or New Yorn. Charles Schuchert, EpirorrAL COMMENT. A New Building for the United States National Museum..... Review or Recent CeroLioaicaLt LirerATuRE. Alphabetical cross-reference catalogue of all the publications of Edward Drinker Cope from 1850 to 1897. Persifor Frazer: . Recent geologic work in Franklin and St. Lawrence counties [iNtexumeViork | Mex slum “\Capshimes ie aie encase al ea Les analyses en bloc et leur interpretation. F. Fouqueé........ 67 112 121 122 123 124 124 125 .127 129 131 135 139 180 181 Contents, Les Roches alcalines caracterisant la Province petrographique d’Ampasindava. A. Lacroix.. Index animalium. C. D. ee bore. ait, URSIN o ecse Das Sonnwendgebirge im TRseeeinrithal< | ein’ Typus alpinien (Pemimecnawesar ir. Po WOUNEr. soi ies i Sl ee ae eke On the lakes of southeastern Wisconsin. N. M. Fenneman.... The origin of certain place names in the United States. Henry SEG EC aa a a TE ee So hte gh St ANC > ae RO ee Bornholms Paradoxideslag og deres Fauna. Karl A. Gronwell Monruriy AuTHor’s CATALOGUE OF AMERICAN GEOLOGICAL LITER- UNTNUIREB,. Guhl BARE Sigh aot ak eth helt Se Ae a a PERSONAL AND ScrentiFic News. The Clayton Stone Axe, 193; Vhomas Crowder Chamberlin, 193; American Museum of Natural History, 193; A new Di- vision of the United States Geological Survey r APRIL NUMBER. Tue Lire AnD Work oF Proressor CHARLES M. Hatt. [ Portrait. ] Op 22 DI TEN TET GGA RE ee 3 Si ae Aes Rees a oe a Proressor JAECKEL’s THESIS ON THE Mone or EXISTENCE OF OR- THOCERAS AND OTHER CEPHALOPopsS. Rudolf Ruedemann.... Wire ANwNorations. John M. Clarke... 0: ci wicee ees ce ae THe CENTRAL Onto Narurat Gas Firzp.! [Plate XIV.] J. A. [BV TRLTOCIALC™ (SCA AEE ORE Kt PER EEE eA ee ee STRUCTURE OF THE SOUTHERN PorTION OF THE KLAMATH Moun- TAINS, CALIFORNIA. Oscar H. Hershey. Ayton ent Some Resutts or THE Late MINNESOTA Buea Seta N. TEES TOTES IES Se Dee nn LES Seo ae Se eR i Review or Recent GrEoLocicAL LITERATURE. Esquisse stratigraphique et petrographique du Bassin de la Tafna. Louis Gentil.. Se eMart toh Rey ete Ellensburg (Washington): foie George O. Smith. ......... United States Geological Survey, folios 81, 82, 83. Messrs. Alden, Campbell, Fuller and Ashley. Sot CY eos Report on the Geology of Louisiana, containing ee in papers by different authors. Gilbert D. Harris, State Geologist, A. C. Veatch, J. A. A. Pacheco.. Notes on Cambrian fintioss G. F. Marthe. with a veve Anton of a new species of Metoptoma............... Bere tira see, Topographic development of the Klamath mountains. J. S. Diller f 5 eet ne ee ae SAS Spud San eee Montuiy AutHor’s eas ALOGUE OF Arent AN eee AL Lirer- ATURE Bye oe PERSONAL AND Seremiieie Neve. Professors Pumpelly and W. M. Davis, 262; Extinct Bison from Alaska, 262; The Geological department of Harvard Uni- versity, 262; A fossil Mammoth’s tooth in Iowa.............. 104 VI Contents. MAY NUMBER. Tue PLEISTOCENE GEOLOGY OF THE CONCANNON FARM, NEAR LAN- sinc, Kansas. N. H. Winchell. [Plate XV-XVIIIL]...... Note on Trranirerous Pyroxene. “Alexander N. Winchell..... Bastn-RANGE STRUCTURE IN THE DeratH VALLEY REGION OF SOUTHEASTERN CALIFORNIA. M. R. Campbell............... EpiIrorrAL COMMENT. How long ago was’ America peopled? ..9. 7) dyin we sehen ee Review or Recent GEoLocicAL LITERATURE. Schmalenseeia amphionura en ny trilobit-typ. J. C, Moberg, The Glacial Geology of New Jersey. R. D. Salisbury........ Montruty AutHor’s CATALOGUE OF AMERICAN GEOLOGICAL LITER- ATURE Meanetee niece uae PERSONAL AND ScieNntIFIC News. Geological Survey of Washington, 325; Am. Phil. Society, 325: The Tetrahedral Theory, 325; Elephant, Bison and Man in Eastern Washington, 325; Mining in Colorado, 326; Har- vard Summer School scholarships, 326; Ellsworth Huntington, JUNE NUMBER. Joun Wester Powe... Geo. P. Merrill . [Portrait:]...-...... Tue RicuhMonp GRouP ALONG THE WESTERN SIDE OF THE CINCIN- NATIT ANTICLINE IN INDIANA AND Kentucky. Aug. fF Poerstays [Plates XOX Xexuil ase nee rate ee eat Eee ieee An otp Piatre CuHannevt. G. E. Condra. ([TWlustrated.]...... | RELATIVE AGE OF THE LANCE CREEK (CERATOPS) Brps oF COoN- VERSE Co., WyoMING, THE JupITH River Brps or MontTaANA AND THE Betty River Beps or CAanapa. J. B. Hatcher.... Tur DETERMINATION OF THE FELDSPARS IN THIN SECTION. J. E. SIL) 1 coe Sci aetna ey halee a ses as. c4 4 Review or Recent GEOLOGICAL LITERATURE. The cause of the Glacial Period, being a Resumé and Discus- sion of the Current Theories to account for the Phenomena of the Drift, with a New Theory by the Author. H. L. True, Existence du Cretace inferieur en argolidt Grece—Existence du Jurassique sup. et de l’infra-cretace dans lisle de Crete, Cle ete.) eV COyeua: Ve. och St Ue ee eee te ees MonruHiy AutHor’s CATALoGuE or AMERICAN GEOLOGICAL LITER- ATURE ei ear MPL TON ea ots DELL ihc, tay Gor MO eNGIO RG, oe 6 CORRESPONDENCE. The Rock Name Anorthosyte. Carl Fred Kolderup........ PERSONAL AND SCIENTIFIC News. Proposed Topographical Map of Michigan, 395; New Mexico School of Mines, 395; Department of Geology of the Univer- sity of Wisconsin, 306; United States Geological Survey, 306; American Institute Mining Engineers, 397; Wisconsin Geolog- ical Survey, 397; International Congress of Geologists, 308; National, Academy. of: Sciences’... >. a eee eee 319 308 THE AMERICAN GEOLOGIST, VOL. XXXI. PLATE I. ae IOCAN GEOLOGIST. Vor. XXXI. JANUARY, 1903. No. I. SKETCH OF THE LIFE AND WORK OF THE LATE Pee SE LW YN; C)M. G. LL. D., F. R. S:, Beans. 2a Cc.. DIRECTOR OF THE GEO- LOGICAL SURVEY OF CANADA FROM 1869 TO 1894. By H.M. Amt of the Geological Survey of Canada. WITH, PORTRAIT, PLATE I. ieee CO. Sclwyn,. C.MeG.,’ LLD., F.R.S:, F.G.S... for twenty-five years the eminent Director of the Geological Sur- vey of Canada, (1869-1894) and one of the original Fellows of the Royal Society of Canada, died in Vancouver, British Columbia, on Sunday, the 19th day of October, 1902, the re- sult of a stroke of paralysis. His death was not altogether unexpected, but it removes from our midst one of the most energetic and active personal- ities in the field of geological work and science in North Amer- ica, Selwyn did much to advance the practical or economic side as well as the highest and fundamental principles on which ge- ology is based. His coming to America marks an era inthe prog- ress of geological thought and investigation inasmuch as he brought with him the practical experience of nearly thirty years of work on the geological surveys of Great Britain and Australia, more especially in the early Paleozoics and the ig- neous masses around which so many minerals of economic value occur, the nature of which he emphasized strongly, and to which he was one of the first to draw special attention and to interpret in their right light. During all the years that he spent in Canada he was diligent in mapping or having mapped the volcanic rocks of the various regions examined. 2 The American Geologist. Janene It is interesting to note that Prin. Dresser’s* paper giving the result of his studies on the petrography of the Eastern Townships of the province of Quebec, issued just at the time of Dr. Selwyn’s death, confirms in a marked degree the anticline theory of the structure of the Sutton mountain and other volcanic belts of that part of Canada. He was the son of the late reverend Townsend Selwyn, canon of Gloucester cathedral, by his wife, Charlotte Sophia, daughter of Lord George Murray, bishop of St. David’s, and grand-daughter of John the fourth duke of Athol. He was born at Kilmington, Somersetshire, England, on the 28th day of July 1828. His studies were carried on, first at home under private tutors, and later he completed his education in Switzerland. At the early age of twenty-one (1845) he was appointed to a position on the Geological Survey of Great Britain under Sir Henry de la Béche. His earliest work on the British sur- vey was under the immediate supervision of no less distin- guished a geologist than A. C. Ramsay. He was one of that contingent of stratigraphical geologists under Ramsay who did so much to lay down the fundamental and carefully traced lines separating the various geological formations in that won- derful compendium of geology that England has proved to be, all in a nutshell: The others on the staff with Selwyn were, W. T. Aveline, Trevor E. James, D. H. Williams, H. W. Bris- tow, and W. H. Baily. Edward Forbes was the palaeontolo- gist, W. W. Smythe, the mining geologist, Sir Joseph Hooker was the botanist, Dr. Lyon (later Sir Lyon) Playfair, the chemist: while Richard Phillips was in charge of the laboratory and museum: with Robert Hunt as keeper of the mining records. Mr. C. R. Bone was employed as artist and C. P. Gibbs as collector of fossils. Under chiefs like Sir Henry de la Béche and A. C. Ram- say, Selwyn made rapid strides in the science of geology for which he had acquired a taste during his stay in Switzerland. He remained attached to the Geological Survey of Great Britain until 1852 and devoted his energies to elucidating and mapping the difficult and intricate structure of the Palaeozoics of North Wales and adjacent portions of western England. *A petrographical contribution to the Geology of the eastern townships of the Province of Quebec.’ Amer. Jour. Sci., 4th series, vol. xiii, No. 70, pp. 43-48. July, 1902. New Haven. Sketch of Dr. A. R. C. Selwyn.—Anu. 3 He is credited with no less than sixteen geological maps prepared either entirely by himself, or, in conjunction with, his chief, Sir A. C. Ramsay, or the Director-General himself, or again, with such well-known men on the geological staff as Ed. Hull, W. T. Aveline, W. W. Smythe, J. Phillips, H. B. Howell and his particular friend and colleague J. B. Jukes. The geological sheets or maps of Leominster, Montgomery, Market Drayton, Harlech, Banger, Bardsey and Machynlleth are ascribed in part or in whole to the subject of this brief sketch). It was during his field work in Wales that Selwyn dis- covered the unconformity between the lowest Cambrian and the older series of schists underneath. In this classic country of the Welsh succession, Selwyn and Ramsay worked together and of one of those ‘Councils’ on the Shropshire sheets the latter wrote at the time in his field note-book :—‘Held a coun- cil with Selwyn on the Shropshire sheets, etc. his work there and here (North Wales) is the perfection of beauty.” “One of the most striking sections of the whole series of sections pub- lished by the Geological Survey,” writes Sir Archibald Geikie later, “runs from the top of Snowdon parallel with the Llan- beris valley to the Menai straits at Llanfair, whence it was afterwards continued across Anglesey. On the other side it was prolonged south-eastwards into the country mapped by Selwyn, and was carried by him into Merionethshire, across Cynicht, Moel Wyn and Aran Moddwy, and was continued by Aveline across Montgomeryshire.” Sir Archibald adds :— “The geological structure is portrayed by Ramsay and Selwyn with a boldness and vigour, and at the same time with an artistic feeling, which had hardly been equalled in geological section-drawing.” In 1845 Selwyn worked out the complicated geology of the voleanic distric of Cader Idris in North Wales: the summer of 1846 he was engaged in mapping out the rock formations in the Dolgelly region, whilst Aveline was tracing the boun- daries of the Silurian series from Llanbrynmair eastward to the Church Stretton and the Longmynd. Ramsay accompan- ied Selwyn and records :— “Glorious days and glorious scen- ery, out with Selwyn along the front of the Cader Cliffs.” He adds :— “Selwyn’s work good.” Testimony from such 4 The American Geologist. January, 1903. a high source must have been very gratifying to young Sel- wyn who rose step by step and advanced in favour amongst his colleagues and superiors. In August 1847 his work lay in the direction of Festiniog in which he was associated with Ramsay, Playfair, Jukes and | Gibbs. This difficult region offered many problems of eco- nomic as well as of geological interest and the careful results obtained were discussed on the ground and incorporated in the classic maps since prepared. The same year Selwyn was at Capel Curig, Jukes was transferred to the South Stratford- shire coalfield and in writing to Ramsay of Selwyn’s work Jukes says :— “It so happens that the last time I saw Selwyn, we were mutually wishing that you would send us both into Stratfordshire together.’ After leaving Wales however the subject of this sketch carried on his investigations in portions of Shropshire as far north as the Triassic outline of Prees. The friendship that had arisen between Jukes and Selwyn in their joint work in Wales grew as years went on; and in 1848 they communicated a paper to the Geological Society of London giving the results of their investigations in North Wales.* This friendship was kept well alive during all the years Dr. Selwyn was director of the Canadian Geological Survey, as many of his colleagues of those years can testify, for, when- ever difficult points in the stratigraphy and paleontology of different portions of Canada arose and were discussed in a forceful and masterly but always courteous and gentlemanly manner, he was wont to quote the words of his friend Jukes as follows :— ‘“‘As my friend Jukes always said, ‘If the palae- ontology does not agree with the stratigraphy, so much the worse for the fossils.’ ” In 1848 Selwyn’s work took him in the Port Madoc and Dolgelly districts of North Wales. There he and. Ramsay pur- sued their work amid the glorious scenery surrounding the heights of Snowdon and the magnificent and bedecked view- points of the foot ranges. In October of that year consider- able discussion arose regarding the ‘structure and succession at Glaslyn, and thither Sir Henry de la Béche, Edward *A.R. SELWYN and J. B. JuKes. ‘‘Sketch of the structure of the country ~ extending from Cader Idris to Moel Siabod, North Wales.”’ rar tery dearaas Geological Society, London, vol. vi, pp. 300- 302, 1848. Sketch of Dr. A. R. C. Selwyn.—Amu. 5 Forbes and also Ramsay went, to determine if possible the points in question and to settle them on the spot. Selwyn was at work on the side of Crib-goch, on the top of a crag, and his well-known shrill shout soon reached Ramsay who discov- ered him, and later in the day they all joined forces and com- pared notes and finally put matters straight at Glaslyn. Many a knotty problem in Cambrian geology was discuss- ed by these masters of geology in the lovely vale of Beddgel- ert where Selwyn was located, or at Llanberis which Ramsay and Forbes made their headquarters. In 1849 Selwyn com- pleted the survey of the rock formations lying between the Snowdon range on the north and Ffestiniog and Tremadoc on the south, and turned his attention to the Lleyn peninsula from Pylheli. At Aber, and as late as. December of the same year, Ramsay and Jukes joined Selwyn and had a very pleasant meeting. The following spring saw the same trio at Merchlyn in North Wales, where many conferences were held on critical points touching sundry lines to be drawn as boundaries between different geological formations. Selwyn was an alpinist or mountain climber of no mean order. From the experience gained when in the Swiss Alps it was a pleasure and no effort for him to climb the peaks and scale the heights of the Snowdon range, not to speak of the numerous crags of the region surrounding the same which he traversed in his geological explorations. Later in life, in the Mount Serle region of South Australia, and in the district surrounding mount Alexander as well as in the Canadian Rockies he was a most intrepid climber. Ramsay. states that he was “out on the hills with Selwyn, one day (4th of May 1850) as far as the cliffs under Carned Llewelyn and down by Mel- ynllyn and Llyndulyn.” Besides good work done on that day “Selwyn executed a most perilous feat of cliff-climbing: a slip and he would have been slain.” Later while in Canada and during the Rocky mountain excursion in connection with the meeting of the British Association for the Advancement of Science in 1884, Dr. Selwyn had a most narrow escape for his life at the mouth of the tunnel near the base of mount Stephen. His keen eye detected the loosening mass of lime- stone above; his agility and wonderful presence of mind led him to jump on adjoining timbers thus saving his life on this occasion. \ G The American Geologist. Janne In the closing months of 1850, after completing the North Wales sections and maps and putting on the final touches in conjunction with Sir Andrew Ramsay, Selwyn was entrust- ed with field work in Anglesey where they crossed and car- ried on the work begun by Sir Henry de la Beche. It was in Anglesey that Selwyn detected the unconformity of the lowest Cambrian strata upon an older Pre- Cambrian series of schists. In this view Sir Henry supported Selwyn, but Ramsay on this occasion differed, so that when the map was published no Pre- Cambrian rocks were shown. In the following year (1851) Selwyn was back at Dolgelly, checking a number of points and investigating critical parts of the complex geological structure. Selwyn was of a bright and cheery disposition and be- sides the happy re-unions held in London on the part of the “Royal Hammerers” as they styled themselves, Ramsay, Sel- wyn, Aveline, Jukes and other geologists of Wales along with their contemporaries, the annual dinners of the Survey were events in which a jolly time was spent: Ramsay in re- cording Selwyn’s presence at. the dinner held 15 January, 1851 says: “And Oh! wasn’t it a jolly dinner!” In 1852 before completing the whole task of mapping the regions examined by him in England and Wales, Selwyn took unto himself a wife, as had also many of his colleagues, mar- rying Matilda Charlotte, daughter of the Rev. Edward Sel- wyn, rector of Hemmington Abbotts, Hunts, and in the fol- lowing year he was appointed by the Colonial Office director of the geological survey in the newly formed colony of Vic- toria, Australia, which had come into great prominence ow- ing to its wonderful goldfields. His training in the older Palaeozoics or Cambrian rocks of Wales was of special value to him in the new colony, and accordingly he set himself to the task of mapping out the gold bearing rocks and auriferous gravels of different ages, and in tracing their relations to other rocks of the district. Here he had a field of work nearly twelve times greater than he had in Wales; Victoria, the smallest of the Australian Colonies, having an area of 87,884 square miles, whilst Wales has a total area of 7,378 square miles only. In Australia Selwyn was ably assisted by Messrs. C. S. Wilkinson, H. Y. L. Brown, C. B. Brown, Robert Etheridge, Sketch of Dr. A. R. C. Selwyn.—Amu. 7 Jr., and other geologists. Besides an extensive series of geo- logically coloured maps of Victoria, and official reports, Sel- wyn prepared the following reports and papers bearing more especially upon the economic resources of Australasia: “On the Geology and Mineralogy of Mount Alexander and the ad- jacent countty lying between the rivers Loddon and Campaspe.” Quart. Jour. Geol. Soc., Vol. X, pp. 298-303. (1854), London. “Report on the Geological Relations of some of the Coal seams of Van Diemen’s Land, their probable extent, and relative economic value.” Van Diemen’s Land Royal Society Papers, III, pp. mw6-I41, 1855-1850. “On the Geology of the Goldfields of Victoria.” Quart. Jour. Geol. Soc., Vol. XIV, pp. 533-38, London, 1858. and Geologist, Vol. I. pp. 163-4. 1858. “Notes on the Geology of Victoria.” Quart. Jour. Geol. Soc., Vol. XVI. pp. 145-50. 1860. Geological Notes of a journey in Australia from Cape Jervis to Mt. Serle,” Proc. Geogr. Soc., Voi..V, pp. 242-44. 1861. “Report on the Auriferous Drifts and Quartz-reefs of Victoria: observations as to the probable age of the Lower Gold Drifts,” Publish- ed in Victoria, Australia, May 4th, 1866. Reprinted in the Geological Magazine, Vel. III, pp. 457-459. London, Eng., 1866. While in Victoria he added much to the knowledge of the gold-bearing rocks of that colony and also aided in tracing the relation of the Miocene Tertiary strata so rich in Eocene Mollusca. Among the interesting collections made by Dr. Selwyn in ‘Victoria may be mentioned that now deposited in the museum of the Geological Society of London, Burlington House, con- sisting of Tertiary shells from the Murray river. He was con- tinuously engaged as director of the Geological Survey of Victoria from 1852 to 1860, a period of nearly seventeen years, _ and he resigned when the legislature refused to vote the ne- cessary funds to carry on the work. Selwyn’s Work in Canada. It was on the first of December, 1869, that Selwyn took charge of the Geological Survey of Canada, which had from its inception in 1842 been carried on by Sir W. E. Logan. Selwyn had arrived in Canada in October of the same year; and vigorously set himself to the task of studying and revis- ing the reports that had been received from the various assist- ants who included the following well-known Canadian geolo- 8 The American Geologist. Janne gists: Sir Wm. E. Logan, Edward Hartley, T. Sterry Hunt, Robert Bell, James ‘Richardson, Charles Robb, and H. G. Vennor. Besides the above, Robert Barlow, Esquire, and his son Scott Barlow, had charge of the topographical and carto- graphical part of the survey, whilst Elkanah Billings was pa- laeontologist, with Messrs. Horace Smith and Thomas C. Wes- ton as assistants, one an artist, the other in charge of museum work etc. When Selwyn became director of the Geological Survey of Canada and deputy head of the same, the confederation of some of the British American provinces had only just been ef- fected, and accordingly there was now open a much wider field of investigation than formerly. As one after another the different provinces and districts became part and parcel of the Dominion of Canada the work increased accordingly, and to such an extent that the staff of geologists and assistants had to be materially increased ; and men had to be trained to pursue the good work of the old régime. This period was one of great activity in the Canadian sur-. vey. The first copies of Logan’s large “Map of the Geology ‘of Canada and adjacent parts of the United States” prepared for the engraver by Robert Barlow, were received during the first month of Selwyn’s administration from Edward Stan- ford, the publisher, Charing Cross, London. As an instance of the remarkable activity and energy dis- played by the second director of the Geological Survey of Can- ada at the outset of his career in Canada, it may be remarked that he not only proposed to the Hon. Joseph Howe the various points noted above but also presented the annual “Summary” report of the geological investigation made by the staff the previous year. He further impressed upon the government the advisability of placing a special appropriation in the estimates of the year for the distribution of Logan’s large map just received, submitting at the same time a list of public and educational institutions, libraries, etc., where the said map would do a great deal of good to Canada. In 1870 he investigated the gold-fields of Nova Scotia and prepared an important report giving the result of his work there. (See. “Report of Progress, Geol. Surv, Canada, 1870- 71,” pp. 352-82, Ottawa, 1870.) Sketch of Dr. A. R. C. Selwyn.—Ami. 9 In the following year, under special instruction from the Hon. Joseph Howe, he undertook an exploration in the re- mote province of British Columbia “On and in proximity to the several lines which will be explained by the engineering parties ‘(of which Mr. Fleming, now Sir Sandford Fleming was engineer in chief,)’ and on one or the other of which the future Pacific railroad will be located.” In the “Report of Pro- gress” for 1871-72, is given an account of the results achieved during these explorations. The route selected by Selwyn took him from Hope on the Fraser via Fort Colville, the Kootenay river and the Columbia to Howse’s pass, and afforded facilities for returning later by wagon-road 378 miles, from Cariboo to Yale. Not only the occurrence of coal-fields, gold-fields and other minerals of economic value, but the timber, soil, water- power, agricultural and numerous other features of special value and interest were also recorded, together with a system- atic description of the various geological formations met with and their relations one to the other in the series from the oldest up. Then in 1872 we find him journeying from lake Superior to Fort Garry, (now Winnipeg) and in the “Report of Prog- ress” for 1872-73 we find no less than three special reports, on the silver mining lcealities on Thunder bay, on the geo- logical investigations from Lake Superior to Fort Garry and on the Acadia iron-ore deposits. In the following “Report of Progress” he gives the result of his observations on the geo- logical exploration in the North West Territories from Fort Garry to Rocky Mountain House. (loc., cit. pp. 17-62.) In the following year Dr. Selwyn remained for the most part of the year in the office, attending to the numerous and onerous duties incumbent upon him and _ preparing for the work imposed upon him in connection with the Canadian exhibit at the Philadelphia “Centennial Exhibition” of 1876. In the “Report of Progress” for 1875-76 pp. 28-31, he gives the summary of personal explorations in British Columbia, and on pp. 31-69 presents his “Journal of the expedition through the Peace River pass.” On pp. 292-93 he adds an important note on a boring made in 1875 on Swan river in the Territory now within the province of Manitoba. He also prepared a map of the region from Quesnel, British Columbia, 10 The American Geologist. Jannat to the junction of the Peace and Smoky rivers. In 1876-77 (Report of Progress for those years) “Notes on the Quebec Group” appear, a subject to which he gave considerable at- tention, and in which he did much to separate from that series those rock formations which were of volcanic origin. In the report of 1877-78 pp. 1-15, further notes are given “On the stratigraphy of the Quebec Group” (of Logan) and older crystalline rocks of Canada. This is said to be one of the best attempts of systematic classification of the most ancient and difficult rock masses ever made. The following year’s report (1878-79) Selwyn’s work in the Eastern Townships and other portions of Quebec is given, and a “Note on the origin of gran- ite treated as metamorphosed strata, not intrusions” occurs in the Report of Progress for 1879-80, pp. 5-6. The same report contains also an account of boring operations in the Souris River valley of.the Manitoba (pp. 1-t1A). On pp. 51-55A the fossil plants collected by Dr. A. R. C. Selwyn at Roche Percée and determined by Sir J. W. Dawson are recorded and de- scribed. His work on the Lake Superior region during the. year 1882 is embodied in the report for 1880-82, pp. 16-17, to- gether with a report on an exploration in Manitoba during the same year on the White Mud and Souris rivers. “On the Geological nomenclature and colouring and no- tations of maps” forms the topic of an important contribution from his pen, pp. 47-51 of the “Report of Progress,” for 1888, followed by additional notes on the geology of the southeast- ern portion of Quebec, pp. 1-7A; and followed later in the re- port by a note on the accuracy of the plan of the mouth of the Moose river surveyed by R. Bell in 1883-84, besides a sum- mary of the work of Selwyn during 1883 on lake Superior, in the Souris Coal district, in Assiniboia and in the Cascade Coal basin of British Columbia. Selwyn leaves behind him a career full of usefulness to the Empire. His work was truly of an imperial nature, for it extended not only into various portions of Great Britain but also to the distant colonies of the mother country, to the “Isl- and Continent” of Australia and to the Dominion of Canada. for nearly eight years (1845-52) he laboured diligently in England and Wales, for seventeen years (1852-1869) he car- ried on geological investigations in Victoria, and spent twenty- / Sketch of Dr. A. R. C. Selwyn.—Amu., II five years additional in Canada thus completing in December, 1894, half a century of active geological work. He was not a voluminous writer for publication, but he was an excellent letter writer. He never spared himself in attending to the nu- merous letters which the correspondence branch of the Geo- logical Survey entailed. He did much! to give the depart- ment the good name it has acquired, and for which it has been so favorably known as a bureau of exact information on a thousand and one things of special interest and value to pros- pectors and investors in all the provinces of the Dominion, as well as in some of the remotest corners of our country. There is little doubt that the state of efficiency of the Can- adian survey grew apace under Selwyn. -Having had for many years closely associated with him as chief advisor and assistant the late and lamented Dr. George M. Dawson, Sel- wyn led the ship through thick and thin most successfully. It cannot be denied that it was under Dr. Selwyn’s administra- tion that the survey reached the hight of its success in carry- ing out the objects and aims for which it was instituted. Nevertheless, it must not be understood that there were no difficulties to overcome, or swords to cross in the long period during which he was director. Selwyn’s aim from the start was to make the Geological Survey of Canada, an eminently practical Department, in which the records of mines and mineral statistics would be kept for the use and information of Parliament and the public. Accordingly, it is with satisfaction that we find him in the second month of his term of office (January 1870) busily en- gaged in organizing a branch of the geological survey for the purpose of collecting in a systematic way “Records of Mines and of Mining statistics of the production and consumption of Minerals in the Dominion.” The decision he arrived at was published in the official “Canada Gazette’ and Messrs. Edward Hartley and Prof. Robert Bell were requested to undertake the collection and arrangement of the returns made from year to year. The inadequacy of the buildings then at the disposal of the survey was a point on which Dr. Selwyn repeatedly dwelt, and a larger amount of the space necessary to the proper illustration and exhibition of the mineral re- sources and industries of the different provinces was repeated- ly urged by him. 12 The American Geologist. da ere His first ‘““Report” is addressed to the Hon. Joseph Howe, M.P., Secretary of State for the provinces, and in it Dr. Sel- wyn points out the practicability of the establishment of a School of Mines in connection with the Geological Survey. The following passage taken from Dr. Selwyn’s inaugural address as president of the section of geological and biolog- ‘cal sciences, of the Royal Society of Canada, delivered May the 25th, 1882, gives an excellent idea of a high-minded spirit. and love of the science to which he was devoting his life and energies. In dealing with general scientific work in new coun- tries and the constant “‘struggle for life’’ which scientists have to encounter, he writes :—‘‘In spite, however, of these difficult- ies Canadian geologists have succeeded in attaining and hold- ing recognized and highly honorable positions in the scientific world. It is needless to dwell on the history and details of the struggle which has achieved this result and in which you all, with others now no more, have nobly shared. It behooves us, however, and especially the younger members of the corps, to remember that the fight is not ended, that, as in the past, so in the future, the struggle will have to be maintained. But if this society so auspiciously inaugurated, effects that much needed concentration, and consolidation of the efforts of the hitherto scattered combatants, uniting them in one solid phal- anx, we may feel assured that the struggle of the future will be a far less arduous one than the struggle of the past. More especially will this be so if we never for a moment forget that the only object of scientific inquiry is truth, That the soul and life of this search in which we are all engaged consists in the fresh interchange of thoughts and the love of full and com- plete investigation, with fair and open discussion, unbiassed by and irrespective of all personal considerations and based not on theory but on carefully observed and honestly stated facts. Such evidence, treated in the spirit I have indicated, certainly will lead us to the truth, but we must always guard against confounding it, as has so often been done, with ingen- ious theory and dogmatic assertion, because these, however clever or eloquently supported they may be, are almost cer- tain to lead us in a direction the very opposite to that in which it should be our aim to travel. For similar reasons partizan- ship, however commendable and necessary in the political Sketch of Dr. A. R. C. Selwyn.—Amu. 13 arena, should never be admitted to the domain of science. Bearing these principles in mind, and above all that unity is strength, I trust that the members of the geological section of the Canadian Royal Society will henceforth be brethren of the hammer not in name only but in very act and deed; that they will at all times cordially co-operate with and assist each other in friendly emulation in the work they have in hand, that of elucidating the geological history, physical and biological,’ of this great country in which the harvest, waiting to be gathered from the rocks, is so abundant but unfortunately the labourers as yet so few.” First and foremost Selwyn was a Sstratigrapical geologist and an able one. He was a firm believer in the field character exhibited by the various series of sedimentary strata in the succession of geological formations in the earth’s crust and _ also by the volcanic materials. He had a special attraction in the regions where the geolog- ical structure was complex and more especially was this the case as regards the eastern townships of Quebec, for, not only during his twenty-five years of office did he take an active part in the examination and elucidation of one of the most difficult and perplexing problems in geology and in the discussions at- tending the same, but even after his retirement he was wont to come back to the survey and to the other members of the staff would present his views in that bold and vigorous man- . ner so characteristic of him. The volcanics of the eastern townships and their associated formations afforded an ex- tensive field for discussion of the highest order. The results of his own field-work led him to interpret the geological struc- ture of that portion of Canada in a manner hitherto unknown on this continent. In the Lake Superior region likewise Dr. Selwyn delighted in carrying on geological investigations whenever the duties of office would permit him to leave the desk for the field. His keen interest in the “Quebec Group controversy” in which Logan, Billings, Hunt, Emmons, Sir Wm. Dawson, Hall, Walcott, Ford, Marcou and many others took a promin- ent part, was ever kept active by the fires arising in the dis- cussion of the numerous knotty points in connection therew th. Selwyn’s interpretation of the geological structure of the so- 14 The American Geologist. TAUB ee called ““Unfossiliferous Quebec Group” seemed a revelation to practical geologists and gave the key to the solution of at least one important side of the controversy, and he thus materially contributed to the advancement of our knowledge of that intri- cate field by separating the volcanic belts; and recognized the anticline structure which they exhibit in contradistinction to the synclinal which the ranges were for many years supposed to present. Like his predecessor in office Dr. Selwyn was always a strong supporter of the Geological Survey Museum not only as an important factor in the interests of the country, but also as an educator. The wisdom of moving from Montreal to Ottawa during his term of office was very soon demonstrated in the numbers who registered and came to it from day to day. The inadequacy of the building and its total unfitness not only for geological work pertaining to the department, but also for exhibition purposes, were time and again emphasized by him and it is no doubt owing to his determination and energy in the direction of preparing plans for a national museum that prac- tical steps have been taken towards the erection of a building worthy of the country. In 1884 a committee of the House of Commons was ap- pointed to investigate the work of the Geological Survey of Canada. The evidence of personal animus displayed by Sel- wyn’s antagonists in the process of the investigation con- trasted with the excellent work that was being done by the Geological Survey in past vears and at the time of the investi- gation led the government to further strengthen the hands. of the director and recommended the establishment of a divis- ion of mines and mineral statistics, much in the lines laid down by Dr. Selwyn himself in 1870, but which for reasons not stat- ed had not been effectively carried out as expected. Selwyn mlet in the Queen Charlotte islands. Selwyn lake, Carr River, Ontario. Selwyn river, Cranberry River, British Columbia, which enters the Fraser river below Tete Jaune cache, are names of places called after the subject of this sketch and serve to per- petuate his name in the geography of the country where his. activities kept him for a quarter of a century. Sketch of Dr. A. R. C..Selwyn.—Amu. 15 Selwyn received many honors in his day. Besides occupy- ing various official and responsible positions appertaining to his office as head of the Geological Survey of Canada in the different international exhibitions which entailed a great deal of executive ability and work, he was created a C. M. G. (com- panion of the Order of St. Michael and St. George) by Her Most Gracious Majesty Queen Victoria, who conferred the honor upon him in person, Selwyn having been summoned to appear at Windsor Castle during the summer of 1886. He was elected a fellow of the Royal Society of England, was one of the original fellows of the Royal Society of Canada, founded by the marquis of Lorne, now the duke of Argyle, and was elected to the presidency of that society in 1896. He also received the medal of the ‘“Acclimatization So- ciety’ of Melbourne, Australia, in 1881. He received the de- gree of doctor of laws (LL.D.) for his distinguished services in the field of geology and was president of the Natural His- tory Society of Montreal in the days when the Canadian Sur- vey was located in that city. In preparing this account of the life and work of our late lamented “chief”, the writer desires to acknowledge his in- debtedness to Dr. Henry Woodward, F.R.S., etc. for his able article on Dr. Selwyn published in the February number of the Geological Magazine for 1899 as one of a series of or- iginal articles on “Eminent living Geologists.” He quoted largely from this source; also from the list of publications is- sued by the Royal Societies of England and Canada, and from N. H. Darton’s valuable “Index” of publications on the geol- ogy of North America, and to Monsieur Michel Mourlon’s “Bibliographia Geologica.” In the office Selwyn was a strict disciplinarian. He loved order and system as well as courtesy and deference due to su- perior officers, such as is the custom in the old world. Neat- ness seemed to be one of his leading characteristics, and in the reports and work that he received from the staff he expected the same. The more stern and severe official side of his nature was in marked contrast with the sociable, amiable and chival- rous which characterized him in his own home; in private and in public gatherings he always strove and appeared to advantage. 16 The American Geologist. Tanna oe. He was tall and graceful, quick and alert, of a rather high- strung and nervous disposition, with a keen and observant eye, capable of grasping the situation at a glance in any emergency: He was economical in his habits; and whilst he was not one of those who bestowed many encomiums nevertheless he duly appreciated work of high order. Selwyn was an English scholar of rare ability. His writ- ings both published and private are masterpieces of English composition, and the time and care that he bestowed upon the various reports and drafts of reports sent in for publication not only added to their value and elegance, but also to the labour devolved upon him; which work might well have been in part entrusted to an editorial staff had the appropriations allowed. Amongst his chief works may be mentioned:—“The Do- minion of Canada and Newfoundland” being Chapter II of Edward Sandford’s “Compendium of Geography and Travel,” a work after Hellwald’s “Die Erde und ihre Volker” published in 1883; “Descriptive Sketch of the Geography and Geology of the Dominion of Canada to accompany the Wall Map of the Geology of Canada,” No. 411, in 1884; Notes and Observa- tions in the Goldfields of Quebec and Nova Scotia. Rep. Prog., Geol. Surv. Can., 1870-71, Montreal, 1872. Bibliography of A. R. C. Selwyn. 1861. Sketch of the country extending from Cadre Idris to Moel Siabod. North Wales, Quart. Jour., Geol. Soc., Vol. IV, 1848. pp. 300-302, Lon- don, England. Prepared conjointly with J. Beetes Jukes. 1866. On the discovery of reptilian footprints in Nova Scotia, Geol. Mag., Vol. IX, 1872, pp. 250-51, London, England. (Selwyn and Ulrich). Geology and Mineralogy of Victoria. 8vo. oI pp. 4 plates, one geological map. Melbourne, 1870. Summary report of investigations dated 7th May, 1870. Geol. Surv. of Can., pp. 1-14. Printed by order of. Parliament, 1870, Ottawa. 1872. Notes and observations on the goldfields of Quebec and Nova Sco- tia. Geological Survey of Canada, Report of progress, 1870-71, pp. 252-282, 1872. Sketch of Dr. A. R. C. Selwyn.—Amu. 17 Report on British Columbia. Geological Survey of Canada, Report of progress, 1871-72, pp. 16-72. Montreal. 1872. Including analyses by 6 tres phen shat Summary Report of Geological Investigations, Geol. Sury. Can., Report of Progress, 1870-71, pp. I-11, (with additional page). 1872. Notes and Observations on the Goldfields of Quebec and Nova Scotia, ibid, pp. 252-282, Montreal, 1872. Summary Report of Geological Investigations. Geol. Surv. of Can., Rep. Progress for 1871-72, pp. II-15. Journal and report of preliminary Explorations in British Colum- bia. Geol. Surv. Can., Report of progress, 1871-72, pp. 16-72. Montreal. 1872. 1873. Summary report of Geological investigations by A. R. C. Selwyn, addressed to the Hon. Jos. Howe, M.P., Secretary of State for the provinces. Geol. Surv. Can., Report of Progress, 1872-73, pp. 1-7, Montreal, 1873. ; Notes on a preliminary Geological reconnaisance from Lake Su- perior to the Winnipeg and English Rivers and to Fort Garry. Geol. Surv. Can., Report of Progress, 1872-73, pp. 8-18, Montreal. Reports upon the Acadia iron ore deposits of Londonderry, Col- chester County, Nova Scotia. Geological Survey of Canada. Report of progress, 1872-73, pp. 19-31, Montreal, 1873. Map. Summary report of Geological investigations. Geological Survey of Canada, Report of progress, 1872-73, pp. 1-7, Montreal, 1873 Notes of a Geological reconnaisance from Lake Superior by the English and Winnipeg rivers, to Fort Garry. Geological Survey of Canada, Report of progress, 1872-73, pp. 8-18, Montreal, 1873. Abstract, Am. Journal Sci., 3d series vol. 7, pp. 517-18 (‘/cp.) 1874. 1874. Summary Report of geological investigations. Geological Survey of Canada, Report of progress, 1873-74, pp. I-09, 1874. Observations of the North West Territory, from Fort Garry to Rocky Mountain House, returning by Saskatchewan River and Lake Winnipeg. Geological Survey of Canada, Report of progress, 1873-74, pp. 17-62, map, 1874. Summary Report of Geological Investigations, Geol. Sury. of Can., Report of Progress, 1872-74, pp. 2-9, 1874. 1875. Age of the lignitic coal formation of Vancouver Island. Am. Jour. Sci. 3d series, Vol. 9, p. 318 (%4p.) 1875. Notes on a journey through the North West Territory from Mani- toba to Rocky Mountain House. Canadian Nat., vol. 7, new series, pp. 193-216, 1875. 18 The American Geologist. Janey ee Notes on a journey through the North West Territory, from Man- itoba to Rocky Mountain House (1874). Can. Nat. and Quart. Jour. of Sci., Vol. VII, pp. 193-216, 1875, Montreal, Canada. 1870. Summary Report of Geological investigations. Geological Survey of Canada, Report of progress, 1874-75. pp. I-23, plate, 1876. Huronian of Canada. Am. Journal Sci. 3d series, vol. 12, p. 461 (4p.) 1876. Descriptive catalogue of collection of the economic minerals of Can- ada and notes on a stratigraphical collection of rocks, 152 pages, Mont- real, 1876. 1877. Report on exploration in British Columbia in 1875. Geological Sur- vey of Canada, Report of progress, 1875-76. pp. 28-86, map, 1877. 1870. . Report of observations on the stratigraphy of Quebec Group and the older crystalline rocks of Canada. Geol. Survey of Canada, Report of progress, 1877-78, pp. tA-15A, Montreal, 1879. Reviewed (J. D. Dana) Am. Journal Science, 3d series, vol. 18, pp. 481-483, 1870. 1881. The stratigraphy of the Quebec Group and the older crystalline rocks of Canada. Canadian Nat., vol. 9, new series, pp. 17-31, 1881. - Reviewed by T. Mcfarlane, pp. 91-102. Report on the boring operations in Souris River valley. Geol. Surv. Can., Report of Progress, 1879-80, pp. 1A-10A, Montreal, 1881. Ab- stract. Phil. Mag., (L. E. & D.) new series, vol. 14, p. 71, (4p.), 1881. 1882. : On the Geology of the Ottawa Paleozoic Basin, Trans. No. 3. Ott. Field, Nat. Club, pp. 34-39, Ottawa, 1881. 1883. On the Quebec Group in Geology. Trans. Roy. Soc. Canada, Vol. I, Sect. 4, pp. I-13, Montreal, 1883. North America. Stanford’s compendium of geography and travel, based on Hellwald’s “Die Erde und ihre vélker.” Maps and illustra- tions, 652 pages. London, Edward Stanford, 55 Charing Cross, 1883. Parts I and II. [Part II, “the Dominion of Canada and New- foundland” by Alfred R. C. Selwyn, F.R.S., pp. 289-636. ] Notes on the geology of the southeastern portion of the province of Quebec. Geol. Surv. Canada, Report of progress, 1880-82, pp. TA.-7A., Montreal, 1883. Geological nomenclature and the coloring and notation of geological maps. Geol. Surv. Canada, Report of progress, 1880-82, pp. 47-51, Mont- real, 1883. On the geology of Lake Superior, Royal Soc. Trans., Vol. I, section 4, PP. E17-122, 4, 1883: The Quebec Group in geology, with an introductory address. Royat Soc., Trans., Vol. I, section 4, pp. 1-13. plate, 4°, 1883. Sketch of Dr. A. R. C. Selwyn.—Ami. 19 Age of rocks on the northern side of Lake Superior. Science, Vol. I, pp. 11. (*/;), 1883. Reviewed by R. D. Irving, pp, 139-140: by T. S. Hunt, pp. 218-19. 1884. Descriptive sketch of the Geography and Geology of the Dom. of Can. to accompany a new Geological Map (Map No. 411). Prepared conjointly with Dr. G- M. Dawson, Geol. Surv. Can., (Separate). Large 8vo, pp. 55. , The copper bearing rocks of Lake Superior. Science, Vol. I, p. 221. 1883. Review of R. D. Irving. pp. 140-41. Reviewed by R. D. Irving, pp. 359-60. (Eastern section). Descriptive sketch of the physical geog- raphy and geology of the Dominion of Canada, pp. 5-26, map, Mont- real, 1884. Abstract, Science, Vol. 5, pp. 156-57. 1884. Notes on observations, 1883, on the geology of the north shore of Lake Superior, (Abstract). Can. Royal Soc. Trans., Vol. 2, sec. .4, pp. 245, 4°, 1885. Abstracts, Science, Vol. 3, pp. 675. 1884. Canadian Rec. Sci., Vol. I, pp. 13-14, 1884. 1885. On the glacial origin of lake basins. British Assoc., Report of 54th meeting, pp. 721-22, 1885. Geological and natural history survey of Canada, Annual Report, new series, Vol. I, 1885. 733 pages, map, Montreal, 1886. Administrative reports by G. M. Dawson, McConnell, Low, Bell, Ells, L. W. Bailey, and Chalmers on geology: Cope on paleontology : Coste on mining laws: and Hoffman on chemical analyses. 1887. The Quebec Group. Science, Vol. 9, pp. 267-68, 1887. Summary report of the operations of the geological survey for the year 1886. Geol. and Nat. Hist. Surv., Report for 1886, Part A, 87 pages, Montreal, 1887. The Huronian of Canada. Am. Geol., Vol. 2, pp. 61-2. 1888. 1888. (Notes on Marcou’s paper, “The Taconic of Georgia and the report on the geology of Vermont.) Am. Geol., Vol. 2, pp. 134-35, 1888. Answer to Dr. Persifor Frazer’s circular, dated Philadelphia, oth May, 1887. (On the subdivision of the Archean, classification of erup- tives in the Archean, unconformities in the Archean, and use of term “Taconic’). International Cong. Geol., Am. Committee Reports, 1888. A., page 55, 1888, Am. Geol., Vol. 2, pp. 207, 1888. (On the use of the term “Taconic”). International Cong. Geol., Am. Committee Reports, 1888B, pp. 17, 1888. Am. Geol., Vol. 2, pp. 207, 1888. On the facts relating to Eozoon Canadense. Science, Vol. II, pp. 146, 1888. Summary report of the operations of the geological survey for the years 1887-1888. Can. Geol. Surv. Reports, Vol. 3, new series, part I, Report A, 117 pages, Montreal, 1888. 20 The American Geologist. ppd p cl 1880. Two systems confounded in the Huronian. Am. Geol., Vol. 3. pp. 339-340, 1889. : Canadian geological classification for the province of Quebec, by Jules Marcou. Boston Soc. Nat. Hist., Proc., Vol. 24, pp. 216-18, 18809. “Annual Report” for the year 1887-88. Geol. and Nat. Hist. Sur. Can. Vol Lie sppy 1-2: 1800. Tracks of organic origin in the Animikie Group. Am. Jour, Sci., 3d series, Vol. 39, pp. 145-47, 1890. The Geology of Quebec City. Science, Vol. 16, pp. 359, 1890. Summary report of the operations of the Geological Survey for the vear 1889. Can. Geol. Reports, Vol. 4, new series, Report A, 66 pages, Montreal, 1800. Tor. (Age of the rocks at Quebec.) Geol. Soc. Am., Bull., Vol. 2, page 501, ISor. 1895. Bibliography of the members of the Royal Society of Canada by John George Bournoit, Secretary of the Society, pp. 70-71, Printed under the Society. May the 25th, 1894. Issued 1895. ; Following is a list of the geological “sheets” or maps, and “horizontal sections” prepared in the whole or in part by Selwyn during the years that he was on the staff of her Majesty’s survey of England and Wales. The maps were published at the ordnance office, whilst the horizontal sections were published at the geological survey office, Jermyn street, London, England. 1848. No. LIX. South East. (Machynlleth), Scale of one inch to a statute mile, London; 1848. Prepared with A. C. Ramsay and W. W. Smyth. : 1850. No. LXXVI. North. (Bardley). Scale of one inch to a statute mile. London, 1859. 1850. No. LXXVI. South. (Bardsley). Scale of one inch to a statute mile. i8so. 1850. No. LXXV. Northwest. (Harlech). Scale of one inch to a statute mile. London, 1850. Prepared with A. C. Ramsay. 1850. No. LV. South West. (Leominster). Scale of one inch to a statute mile. London. 1850. Prepared with W. T. Aveline. 1850. No. LXXV. South West. (Harlech). Scale of one inch ot a statute mile. London, 1851. 1852. No. LXXVIII. South West. (Bangor). Scale of one inch to a statute mile. London. 1852. Prepared in conjunction with A. C. Ramsay and W. W. Smyth. 1852. No. LXXVIII. North West. (Bangor). Scale of one inch to a statute mile. 1852. Prepared in conjunction with Sir Henry de la Béche, W. W.:Smyth and A. C. Ramsay. Sketch of Dr. A. R. C. Selwyn.—Anmu. 21 ‘1852. No. LXXVIII. South East. (Bangor). Scale of one inch to a statute mile. London, 1852. Prepared in conjunction with A, C. Ram- say, W. T. Aveline, J. B. Jukes. 1852. Horizontal sections, Sheet No. 26. Geological Survey of Great Britain. Scale of six inches to one mile. London, 1852. Published at the Geological Survey Office. Prepared conjointly with W. T. Aveline. 1853. Horizontal sections, Sheet No. 29. Geological Survey of Great Britain. Scale of six inches to one mile. London, 1853. Publish- ed at the Geological Survey Office. Prepared conjointly with A. C. Ramsay and W. T. Aveline. 1853. Horizontal Sections, Sheet No. 28. Geological Survey of Great Britain. Scale six inches to the mile, London, 1853. Published at the Geological Survey Office. 1853. Horizontal Sections, Sheet. No. 28. Geological Survey of Great Britain. Scale six inches to the mile. London, 1853. Published at the Geological Survey Office. Prepared conjointly with A. C. Ram- say. 1853. No. LXXV. North East. (Harlech). Scale of one inch to a statute mile. Prepared conjointly with A. C. Ramsay, W. T. Aveline and J. B. Jukes. London, 1853. 1854. Horizontal Sections, Sheet. No. 37. Scale six inches to the mile, Geological Survey of Great Britain. Prepared jointly with A. C. Ramsay and W. T. Aveline, London, 1854. 1854. Horizontal Section, Sheet 31. Geological Survey of Great Britain. Six inches to the mile. London, 1854. Prepared jointly with A. C. Ramsay, J. B. Jukes and W. T. Aveline. 1855. No. LV. South East. (Leominster). Scale one inch to the mile. London. 1855. Prepared jointly by J. Billups, W. T. Aveline and H. B. Howell. 1855. No. LXXIII. South West. (Market Drayton). Scale of one inch to a statute mile. Geological Survey of England and Wales. Lon- don, 1855. Prepared jointly with Edward Hull. 1855. No. LXXIII. North West. (Market Drayton). Scale of one inch to a statute mile. Prepared jointly with Edward Hull. London, 7855. 1855. No. LXIII. South East. (Market Drayton). Scale of one inch to a statute mile. Prepared with Edward Hull. London, 1855. 1855. No. LX. North West. (Montgomery). Geological Survey of Great Britain. Prepared jointly with J. B. Jukes, W. T Aveline, and Sir A. C. Ramsay. London, 1855. 1857. No. LXXTII. North East. (Market Drayton). Geological Sur- vey of England and Wales Scale of one inch to a statute mile. Pre- pared jointly by W. W. Smyth and Edward Hull. London, 1857. to to The American Geologist. Beesintses 8 ON RHOMBOPORA LEPIDODENDROIDES MEEK. By G. E. Conpra, PH. D., Lincoln, Neb. PEATE Il, EIGS. 1-10, ~ 1866. Stenopora columnaris. Geinitz (not of Schlotheim, 1813, (in part) Carb. und Dyas in Nebraska, p. 66. ‘1872. Rhombopora lepidodendroides Meek, Pal. Eastern Nebr., p. 141, Pl. VII, 2a-f. 1877. Rhombopora lepidodendroides (?). White, Wheeler’s U. S. Ge Shy HAWG BIG, oy oly Jed NI S eal, 1884. Rhombopora lepidodendroides. Ulrich, Jour, Cincinnati Soe. Nat. Hist., VIL, p. 27, Pl. I, 1-1b. 1887. Rhombopora lepidodendroides. Foerste, Bull. Sci. Lab., Den- ison Unive it, p73, Pl VIL 3a, _b: “1888. Rhombopora lepidodendroides. Keyes, Proc. Acad. Nat. Sci., Philadelphia, p. 225. 1894. Rhombopora lepidodendroides. Keyes, Missouri Geol. Surv., Vo piegs, Plex XT aa. th, » 1896. Rhombopora lepidodendroides. Smith, Proc. Amer. Phil. Soc., XXXV, p- 237. 1899. Rhombopora lepidodendroides (?) Meek. Knight, Jour. Geol., VII, p. 366. ‘1900. Rhombopora lepidodendroides Meek. Nickles & Bassler, Bull. gy AUB SA Eos, (108 SO . 1901. Rhombopora lepidodendroides. Rogers, Kans. Univ. Quar., IX, No. 4, pp. 240, 241, 245. Among a very large number of Coal Measure fossils found in Nebraska, some of which have been of service in determin- ing stratigraphy, the following seem to be the most common and widely distributed: Fusulina secalica, Seminula argentea, Chonetes granulifer, Spirifer cameratus, and Rhombopora lepidodendroides. The last named species has a wide range both vertical and horizontal; it is more or less plentifully found in nearly all Coal Measure exposures of the state, and in the Permian at Blue Springs and Wymore. The first specimens were collected from outcrops along the Missouri river by professor Marcou. They were identified by professor Geinitz of Dresden, in 1866 as Stenopora colum- naris (Schlotheim 1813, in part). According to Meek, who named the species in 1872, the specimens observed by Geinitz were R. lepidodendroides Meek encrusted by Fistulipora nodu- lifera Meek. The writer has found several specimens which were quite concealed by Fistulipora nodulifera Meek. It is very THE AMERICAN GEOLOGIST. VOL. XXX1. PLATE IT. speapcsatas ia Dai mr te <—es ve; xt en ret tae Cot ET RHOMBOPORA LEPIDODENDROIDES. ot 1 as f % P| y aah he hay"! mA a 1 la 7 dl ’ ] "> v7 wre te Th f hay) yb hy 7 ; | mie), hh eee yaa) ver, hen aye Melee ak ein PRL ena? Ng iy ery) hy TY) cot i Nb aR a 1 en " i ae ure of > i eat Nkayy »? Aaihs a ye ° ’ , ya Ci fs iv* [ : - 7 iAP j a 4 / i ofl ' phd } ' "ad ‘ 7 e Pawe : , | 7) a! a iT, Ty ¢ ol 4 R i ' , ¥ y F| : : sal er" a4 , 7 ore Te a ae gl ( tate OPT bape! cate a ' n 1 nM 1 . A > i mi ’ i id eA 1 7 e : * uf wu 4 ;* J ; k ' a, ‘ Z eek, ra \ vil “ile, Eee es / id Gr Se San Te a en : vidi, rae ; ‘ ft less hy ; 3 : 5 f ell WA oe ON EN ee ath ina oe a eh itera) 1 se gS eau; pee er f ehh. gh eS [a . AB anh) a NE Le ob altos i oh bs ea Beene eae i Ser tac ri DS) eee ye : he By at ae mie hes { en i= : ; , ae ; “\ ld) ¥ tag ‘ lie 7 . / i ye ; { \ { i Ly ; 1 Na ay i i \ ae P ' ek " Bou ( ’ r WP ; »y : ‘ ’ ra vy 2 ‘ 1 s , 1 : i ean - A “ [ ‘= * 4 ~ Ms . . ’ ‘w \ 9 i ‘ i Lee be - ian \ d > y i - hate Ne j Nyy . @ any , at " f fe® | rib y j - i ; ; ’ ky i : * "4 = ~ / ih i / \ | .) i i +f oat ¥ 1 ‘ a + ' i f 70 " ’ J 4 Pail / 7 d- RS if o = y . 1 ; 7) ' aft , 1 ti * J 2 i fa) \ F | ; = f i, ‘ j i A \ j oF ' . i ' i f ; , ‘ yi j* } a 5 , x : wei , | i / i ® = y ' y , ] y ) ; ! “4 , i uf ' : ' ; ln 7 ‘_ i i / * ri " i F) ‘ " . A } Le i" P + ‘ he ‘ey ‘ i} r £ ’ .. y ; b f On Rhombopora Lepidodendroides Meek.—Condra. 23 evident, therefore, that professor Geinitz may have erroneously identified two new species, One covering the other, as a single described species. The object of this brief paper is to announce the positive occurrence of the species in the Permian of Nebraska, and to briefly delineate its different forms of growth, only one of which has been described. Meek’s diagnosis is based on the young growth, and, as a result, the species is often imperfectly known by that form alone. The writer has collected and placed in the museum of the University of Nebraska not less than fifty pounds, representing several thousands, of nice clean specimens. They fall under the following growths: 1, young form; 2, old non-montiferous form; 3, old montiferous form, Lo these may be added the encrusting form which is rarely tound. From superficial characters, the casual observer would try separate the specimens into as many species as there are forms of growth. Description.—Zoaria ramose, rarely encrusting, ‘cylindrical or slightly compressed, straight to irregular in extent between bifurcations, in young and old forms; surface smooth or mont- iferous ; bifurcations at irregular intervals, equal or unequal in size, angle variable, usually 60 to 80 degrees. Young forms (figs. I, 2, 9, 10.) slender, cylindrical, small, average diam- eter less than 2 mm., surface papillose, due to projecting acan- thopores. Old forms (figs. 3-6, 8, 11.) larger, more irreg- ular, with or without monticules, size variable, diameter 3 to 8 mm., average 4 Or 5mm.; monticules of montiferous form differ in size and arrangement as shown by fig. 5. Zooecia curve gradually from central to cortical portions of zoarium, through which, in old growths, they continue in near- ly straight lines to the apertures; walls in central or immature region thin, in cortical or mature portion thick with acantho- pores as a prominent feature; acanthopores or tubuli, as they are sometimes called, between zooecial walls, ot two sizes, large and small, projecting from the surface when well pre- served. Zooecial cavities or cells polygonal in the immature region, circular in section and usually smaller in the mature portion. Tabulae wanting in most cells, but frequently found in old forms. Apertures subcircular in forrn, arranged (in young growth) in vertical and diagonally intersecting series 24 The American Geologist. January aie which open into rhombic or subelliptical vestibules; Vestibules in very young specimens subelliptical. The intersecting series and vestibules are not plainly shown in old forms. These brief notes may show that the so-called rhombic vestibule has been overestimated as a character. | Probably the encrusting form has been described as a species under Stenopora. The systematic position of the species is held in dispute. Meek placed it under the polypi. Position and locality—Coal Measures: “A rather common species at various localities in Nebraska, Kansas, Missouri, Towa, Illinois, and Ohio.” Found at Bennett, Roca, Ashland, South Bend, Louisville, Richfield, Cedar Creek, Plattsmouth, Wyoming, Nebraska City, Tecumseh, Table Rock, Humbolt, Dawson, Salem, Falls City, Weeping Water, Nehawka and other localities in Nebraska. The young form occurs in large numbers at Table Rock, while the old forms are even more plentifully found just above a thick bed of flinty limestone outcropping along the Platte river from Louisville to South Bend. Permian: Some years ago professor Knight collected specimens at Blue Springs and Wymore and referred them with question to this species. Since that time the writer has identified the species in the Florence flint at those places. Professor Prosser has collected and identified specimens from the Permian of Kansas. EXPLANATION OF FIGURES. Young form outlined natural size. Young form, transverse section, outlined natural size. Old non-montiferous form, outlined natural size. Old ‘non-montiferous form, outlined natural size. Old montiferous form, outlined natural size. Old montiferous form, transverse section, outlined natural size. Young form, surface enlarged, showing vestibules with large acanthopores at the vestibule angles. 8. Old non-montiferous form, tangential section from mature region, 9. Young form, transverse section of zoarium. 1o. Young form, vertical section showing transition from immature to mature region as well as form and size of cells. 11. Old non-montiferous form, vertical section showing walls, tab- ulae, and cells. Note.—Figures 9, 10 and 11 were drawn by Miss E. P. Hensel. Oo N 4 N Ou & Valley Loess of Lansing, Kan.—U pham. 25 VALLEY LOESS AND THE FOSSIL MAN OF LANSING, KANSAS.* By WARREN UPHAM, St. Paul, Minn. The deposition of the loess in the Missouri and Mississippi valleys, forming a most important part of the modified drift supplied from the waning continental ice-sheet, was very di- rectly dependent on a widely extended depression of our vast glaciated area, which, from a later part of its records in the basin of Lake Champlain and the St. Lawrence valley, has been named the Champlain depression, characterizing the clos- ing stages or Champlain epoch of the Ice age. Looking to the causes of the snow and ice accumulation, which prevailed during a relatively long time, attended, however, with great fluctuations of the ice borders, and to the opposite causes of the final departure of the ice-sheet, which occupied compar- atively only a short time, we find the Glacial period divisible into two epochs. The first was a time of high elevation of the lands which became glaciated, as known by river valleys on the continental borders now very deeply submerged beneath the sea. Snowfall, instead of rain, predominated throughout the year, giving a general though wavering growth of the continental icefields, with prolonged work of drift erosion and transportation. This was the Glacial epoch, as we may term it, comprising the far greater part of the Glacial period. But it is less fully known, as to the details of its history, than the ensuing Champlain epoch of depression of this glaciated region, when the ice-sheet finally melted away, albeit with many vicissitudes of halting and even occasional readvance interrupting the glacial retreat. In this epoch, begun by the Champlain subsidence of the land beneath the immense burden of the ice-sheet, the earliest deposits were the loess of the Missouri and Mississippi region and the nearly analogous white silts on the area drained by the Ohio river. With abundant melting of the icefields which supplied these very extensive modified drift beds, the weight pressing down this part of the earth crust was much diminished, allowing it to rise probably 300 to 500 feet in this great in- * Presented at the meeting of the A. A. A. S.in Washington, Jan. 2, 1903. 26 The American Geologist. January, 2o8e- terior region, adjoining the northern ice-sheet, so that when the somewhat later knolly and hilly marginal moraines were amassed along its boundaries at pauses of its recession, a coarser modified drift formation of sand and gravel was spread along the river valleys by the stronger and faster flowing streams that then received the drainage of the ice melting. The valleys had already been reéxcavated from their filling of loess. New floodplains of gravel, sand, and silt, brought by the waters from the ice melting and rains during the Wisconsin or moraine- forming stage, attained great thickness near the ice borders, but thinned more rapidly southward, so that their continua- tions in the great valleys are now covered, or have been mostly worked over and redeposited, in the Postglacial alluvium. As fast as the ice-sheet withdrew and left the land bare, it was reelevated farther north to nearly the same extent of a few hundred feet as before in the upper Mississippi region. A wave of permanent uplift thus advanced toward the central area that was last occupied by the icefields. Not many thous- and years, probably, after the loess areas were uplifted, the basin of the vast Lake Agassiz, now represented by Lake Winnipeg, was reelevated, rising mostly 300 to 500 feet at the rate of about a half of a foot yearly, by a gradual move- ment advancing from south to north; at nearly the same time, the coast of Maine and the Champlain and St. Lawrence valleys were uplifted to a similar amount; and in the north central area of our continent, including Hudson bay, the uplift still appears to be in progress, averaging for some districts per- haps as high a rate as three to five feet or more in a century. The loess region may have been wholly raised to its present hight far more rapidly, like the Lake Agassiz basin, within a thousand years, permitting the erosion of the loess to take place very soon after its deposition. No longer interval than a few thousand years may therefore have separated the Iowan stage of loess deposition, with its very slow river currents, from the Wisconsin stage of moraine accumulation and attendant trains of gravel and sand washed down the valleys by rapid streams. The admirable investigation of the physical and chemical characters of our loess deposits by Chamberlin and Salisbury in the paper of their joint authorship, “The Driftless Area of the Upper Mississippi Valley,” published in the Sixth Annual Valley Loess of Lansing, Kan.—U pha. 27 Report of the United States Geological Survey, 1885, leaves no ground for doubt that the loess of the Mississippi and Missouri valleys was derived mainly from the North American ice-sheet, being a deposit of the flooded rivers during a stage of very abundant ice-melting, with considerable redistribution over the interfluvial upland areas by winds. Several years later, an equally important work by McGee, ‘The Pleistocene History of Northeastern Iowa,” appeared in the Eleventh Annual Report of the same survey, presenting most satisfactory and conclusive evidence that the chief stage of plentiful and rapid deposition of the loess was when the ice-sheet still covered a large part of Iowa and stretched thence very far northward, but after it had relinquishd the outer area of its drift which extends south to central Missouri and northeastern Kansas. : Paha, or eskers of loess, described by McGee, and broad swells and embanked ridges of loess, also described by him and by Calvin, amassed along the border of the ice-sheet at its Jowan stage, rising 20 to 50 feet or more above the adjoin- ing almost perfectly level expanse of till on which the ice lay at the time of these loess accumulations, give me a complete assurance that the loess’ there was supplied principally from englacial drift which at last became superglacial by ablation or surface melting. As with the more common types of eskers and kames, composed of coarse and fine gravel and sand, I am obliged to refer these loess formations to streams flowing down from the dissolving ice surface, not upward-from subglacial tunnels. They go with the numerous arguments of Profs. N. H. Winchell and W. O. Crosby, and of the present writer, to prove that the departing North American ice-sheet, when its thickness near the margin was greatly reduced, became cov- ered there by the drift which had previously been enveloped within the slowly flowing ice, nearly as the Malaspina ice- sheet or piedmont glacier in Alaska, between Mt. St. Elias and the ocean, is covered by its formerly englacial drift, on which are now growing forest trees of large size and luxuriant thickets. Similarly the Greenland ice-sheet, if it were melt- ing away instead of increasing or remaining nearly unchanged, would become covered at its border by the drift of its basal part, then becoming superglacial. 28 The American Geologist. Janay ee On the melting and drift-bearing margin of the ice in the Missouri, Mississippi, and Ohio basins, where a great propor- tion of the drift is very fine-grained, with usually an appreciable calcareous element, from erosion of limestones or of the fre- quently calcareous shales of the great Cretaceous areas west of the Mississippi, the superglacial drift, washed by the streams of the ice melting, and of the accompanying copious rains, yielded to the rills, brooks, and rivers discharged from the ice surface, a very abundant freight of fine muddy silt, usually somewhat calcareous. Being laid down in the ice-walled chan- nels of the streams near their debouchure to the open ground, or along the edge of the icefields, this modified drift is pre- served to our time in the very instructive loess paha, and in the high loess embankments and slopes that fringe the outer boundary of the Iowan till expanse. What conditions produced and controlled the deposition of the valley loess? First, this region was differentially de- pressed, with all the North American area of glaciation, until it stood lower than now, the maximum reélevation in the Mis- — sissippi basin being, as I think, about 500 feet, or, according to the estimate of Chamberlin and Salisbury, probably as much as 800 feet. (The physical characters of the earth crust, and of the plastic or molten interior, which could admit such dif- ferential movements, I discussed eight years ago in Mono- graph XXV of the United States Geological Survey, entitled “The Glacial Lake Agassiz.’’) Second, with restoration of a temperate climate on the border of the ice-sheet, brought by the subsidence from the formerly high elevation, extensive surface melting of the ice exposed its englacial drift, much of which was washed away and borne into the valleys beyond the ice boundary. The very fine modified drift in the Mississippi region, called loess, could be carried by the gently flowing streams far along the great valleys, in which it formed thick floodplain deposits, the swollen rivers being uplifted on them to hights of 150 to 250 feet above their present beds. Today the Missouri is sometimes called “the Big Muddy,” a name which it well deserves, for at all seasons a white plate lowered into its muddy current becomes invisible within ‘a depth of two or three feet. But ‘during the final melting of the ice-sheet this river Valley Loess of Lansing, Kan.—Upham. 29 and all the others of this basin were much bigger and much muddier. Though flowing with slackened currents on account of their decreased slope, they carried the fine particles of the loess hundreds of miles down the Missouri and Mississippi valleys, building up wide and thick floodplains as far south- ward as to Crowley’s Ridge in Arkansas, and even onward past Vicksburg and Natchez, thinning out on the shores of the Gulf. During the summers of each year the floods pouring along the vallevs from the ice melting and rains added a little to the surface of the whole floodplain; but in the autumn, winter, and spring, the diminished rivers flowed in comparatively narrow channels, probably permitting the main part of the floodplain to become more or less covered by grass and other vegetation and to be inhabited by air-breathing mollusks. Hence,. even in the vallevs, the fossil shells of the loess are mostly of terrestrial species. Jf a quantitative estimate of the average rate of deposition of the loess in the valleys be at- tempted, I think two or three inches of added thickness in the three or four summer months of the river floods in each year to be perhaps a reasonable supposition, which would re- quire a thousand years, approximately, for the accumulation of the depths of 150 to 250 feet. From the very extensive tracts of the floodplains, several or many miles broad and reaching along the valleys hundreds of miles, the winds in the cooler part of the year, when these ereat expanses were bare, blew away much of- the fine loess dust and spread it far and wide over the interfluvial higher lands. Received there on a grassy surface, like that of our present prairies, the loess settled from the gales and mantled somewhat uniformly all the land, regardless of its contour or altitude. In these great areas of eolian loess only terrestrial shells are found. Here again we may essay an estimate of the rate of deposition, assuming that the wind action might bring on the average a sixth or a quarter, or even a third, of an inch in thickness vearly, so that within the same thousand years of the valley loess formation the observed interfluvial locss sheet, mostly 10 to 25 feet thick, would be distributed in its surpris- ing uniformity over the high and low lands alike. } _ Nor were the winds limited to the river floodplains for the derivation of their loess dust. On the drift-enveloped border 30 The American Geologist. J ey ee of the ice-sheet, which probably differed from that of the Mal- aspina glacier by having commonly neither trees, grass, nor any vegetation, the gales in dry weather could gather much of this very fine silt, sweeping it off high in the air to be deposited far away with the other interfluvial loess. It should also be added that this silt mantle doubtless includes some contribution, most considerable westward, of dust from the great western plains, this part being not of glacial origin. According to the well known investigation and report of Humphreys and Abbot, the silt deposited annually by the Mis- sissipp1 beyond its mouths and on its delta and swamp lands would cover a square mile to the depth of 315 feet. Ina thousand years, therefore, at its present rate, the river deposit at and near its mouths would be equal to the measure of a thousand miles in length, two miles in width, and nearly 160 feet in depth. During the rapid glacial melting of the Iowan stage, however, we may reasonably suppose that the mean annual volume of the Missouri and Mississippi was twice or three times as great as now, its foods being prolonged through- out the summer; and the amount of silt gathered from the melt- ing ice-sheet may have averaged fivefold, I believe, or per- haps for some centuries even tenfold, more than the present supply. It seems therefore, by comparison with the work of these great rivers now, that they were competent, when the Champlain subsidence favored rapid melting of the ice, with an abundant supply of silt and very gentle slope of the stream courses beyond the ice border, to deposit the valley loess in the manner and time here indicated. Afterward, too, when the region was somewhat reelevated as at present, it is evident that the reéxcavation of the valleys would require only a few thousand years to deepen them, as before the moraine-forming Wisconsin stage, to levels below the bottomlands of today. My principal motive for this study of the loess comes from the discovery, in February of last year, by the Messrs. Con- cannon in a tunnel cellar on their farm near Lansing, Kansas, of a human skeleton beneath the lower part of the valley loess of the Missouri river, as I regard the geologic section there.* * AM, GEOLOGIST, vol. xxx, pp. 135-150, with two plates, Sept., 1902. The same number also contains, in pages 189-194, an editorial article on this sub- ject, by Prof. N. H. Winchell, including notes on the Lansing skeleton by Prof. S. W. Williston. Valley Loess of Lansing, Kan.—Upham. 31 This locality was visited by Prof. N. H. Winchell and myself, with others, August 9th. Six weeks later, September 2oth, it was visited by Profs. W. H. Holmes, T. C. Chamberlin, R. D. Salisbury, and Samuel Calvin, with others; and a long article by Chamberlin, with short statements from Calvin and Salis- bury, has been since published.* Extensive excavations were made there within the next month by Mr. Gerard Fowke, under the direction of Prof. Holmes, to obtain additional ob- servations of the characters of the deposits overlying the skel- eton. The result of this investigation is regarded by Cham- berlin, Calvin, and Salisbury, as adverse to the conclusions before announced by Winchell and the present writer, which referred the fossil man of Lansing to the Iowan stage of the Glacial period. Instead, they consider him to be of much less antiquity, the overlying 20 feet of silt being thought to be Postglacial alluvium from the drainage area of a little trib- utary ravine which there joins the great Missouri valley. Against this view I see two decisive objections, which seem to me sufficient to necessitate the reference of the Lansing man to the loess-forming Iowan stage of glaciation... First, the overlying silt, regarded by Winchell and myself as loess, is predominantly calcareous in nearly the same degree as av- erage loess, though it has some scanty portions that have very little calcareous matter or none; whereas if it were a Postgla- cial deposit, whether by the Missouri river or the adjoining ravine, or by both together, its material, derived from the weathered and leached superficial part of the loess, from the old Kansan drift thinly spread in that region, and {rom the weathered Carboniferous strata, would be mostly destitute. of its calcareous ingredient. But the proximity of the ravine, of the Kansan drift, and of the Carboniferous limestone and shale beds, gives an ample explanation of the scanty inter- mingling of materials of local derivation with the otherwise typical loess. While the old floodpain of the Iowan time was being deposited at the horizon of the Lansing skeleton and for the next twenty feet upward, exceptionally heavy local rains, and the snow melting in spring, would sometimes carry down an alluvial deposit of silt from the ravine, or pebbles and larger * Journal of Geology, vol. x, pp. 745-779, with 13 illustrations in the text Oct.-Nov., 1902 (issued about Dec. 5). 32 The American Geologist. Janae eae rock fragments, such as are inclosed in this section and in most other sections of loess adjoining the rock bluffs of the valley, especially where it receives a small tributary. In this connection we may notice that the Concannon tunnel in its outer half, dug during the winter of 1900-1901, had perfectly maintained its vertically cut sides and slightly arched top a year and a half before our visit, behaving in the manner so characteristic of the loess, which would not be possible in any Postglacial deposit of alluvium. The second objection to Chamberlin’s view relates to his assumption that the Missouri river during some part of the Postglacial period had a floodplain at Lansing about 25 feet above that of the present time. Changes then taking place as to the course of the river’s channel are supposed to have per- mitted the stream in the ravine to deposit the silt above the skeleton. On the contrary, if I rightly read the geologic his- tory of the Missouri and Mississippi rivers, the floodplain at ‘Lansing and southward was lower during the Wisconsin stage of glaciation than now, and has in general been somewhat built up, instead of being cut down, during all Postglacial time. With the uplift of this region which preceded the form- ation. of the Wisconsin and Minnesota moraines, the valleys ac- quired their present slopes, and the valley loess was rapidly eroded. Its deposit along the Missouri, once having the hight of probably 150 feet above the Lansing skeleton, was removed, giving the valley its present width and even a greater depth than now, before the moraine-forming stage of the waning Ice age. During this process of reexcavation, the remnant of loess at and above the Concannon tunnel was spared; and here and there, as close north of Council Bluffs, a terrace wouid be left midway between the crest of the valley loess bluffs and the present bottomland. Sufficient time intervened between the Towan and Wisconsin stages to allow the great valleys to be sculptured in the easily eroded loess to nearly their present form with a somewhat greater depth. Through this interval the ice accumulation and melting were almost evenly balanced ; but there next ensued a time of general and prolonged re- cession of the ice border, interrupted by many halts shown by parallel and partly interlocking moraine belts. From the abun- dant melting of this Wisconsin stage, floods again poured Valley Loess of Lansing, Kan.—Upham. 33 along the valleys and deposited much modified drift. They descended with the same valley slopes as now, and their strong currents bore the finest silt far southward, to the lower Mis- sissippi and the Gulf, while the gravel and sand were deposited along the upper part of the valleys. In the close vicinity of the moraines the outwashed coarse modified drift filled the valleys 100 to 200 feet, or more, above the present rivers; but the fine clayey silt borne farther down the valleys was deposited in much less volume than the earlier loess, being mostly swept on by the river floods to the Mississippi delta. Along the Big Sioux valley, on the northwest boundary of Iowa, a floodplain of modified drift associated with the moraines has an average width, as described by F. A. Wilder, of one and a half miles, and is about ten feet above the present relatively insignificant bottomland, which averages only about a fifth of a mile in width.* Below the junction of the Big Sioux with the Mis- souri, this floodplain of Wisconsin time continues with a width of 6 to 12 miles on the east side of the Missouri through the distance of 90 miles to Council Bluffs and Omaha, having only the same slight altitude above the river. Southward from the mouth of the Platte river, as [ think, the old Wisconsin floodplain was lower than the bottomland today, which has evidently gained in depth, rather than lost, ever since the Ice age. Conditions requisite for silt deposition 30 to 50 feet above the Missouri at Lansing appear thus not to have existed since the Iowan loess was spread deeply along this valley. It seems needful to add only a few words more. The an- tiquity of the Lansing man I think to-be measured by about 12,000 years, or, at the longest 15,000 years; and this is prob- ably the earliest evidence of man known in relation with depos- its referable to glaciation in America. The stone arrowhead not- ed by Willistont as found with the bones of an extinct species of bison in western Kansas is undoubtedly about equally old. But the stone implements and human bones found by Ab- bott, Putnam, Volk, and others, in glacial gravels at Trenton, N. J., belong to a later stage in the departure of the continental ice-sheet. Probably almost contemporaneous with these are the evidences of early man made known in modified drift deposits * Towa Geol. Survey, vol. x. 1900, p. 142. + The Unversity Geological Survey of Kansas, vol. ii, 1897, pp. 297-308. AM. GEOLOGIST, vol. xxx, pp. 313-315, with section, Nov., 1902. 34 The American Geologist. danuaky meas of Ohio by Wright, Mills, Claypole, and others, and in the upper Mississippi floodplain of the end of the Glacial period at Little Falls, Minn., by Winchell and Brower; which, in their turn, antedate the prehistoric hearth in New York under a beach of the glacial Lake [roquois, reported by Gilbert, and the artificial flakes of stone noted by Tyrrell in a beach on the northwestern shore of lake Agassiz. These all belong, how- ever, to the closing stages of the Ice age, probably ranging from 9,000 to 7,000 years ago. The men of Lansing, and of these later modified drift and lacustrine deposits, were very near our own times in comparison with the antiquity well known for man in Europe. In the Old World man has existed at least 100,000 years, and not improbably even twice as long. In America he may have had 50,000 or 100,000 years for the origin of the physical characters of the American race. There- fore the resemblance of the Lansing skeleton to the average type of our American aborigines, called Indians, appears in no degree surprising to one who believes that the creation of plants and animals has proceeded by the gradual methods of generic and specific development which are collectively termed evelution. NOETLING ON THE MORPHOLOGY OF THE PEEECY PODS: By RUDOLF RUEDEMANN, Albany, N. Y. PATE Le The most recent of Mr. Noetling’s papers on the pele- cypods introduces an element so novel and promising of useful- ness into the morphology of the pelecypods, that we wish to aid in making it known to the American students of paleon- tology. The author admits that he owes the incentive to his investi- gation to Jackson’s suggestive work on the “Phylogeny of the Pelecypoda,” in which Jackson establishes the peculiar fact of the torsion of the hinge line in reference to the body of certain pelecypods, but, as Noetling claims, fails to recognize the importance of the discovery, and also considers the axis * FRITZ NOFTLING: Beitrage zur Morphologie der Pelecypoden. Neues Jahrbuch fur Min. Geol. & Pal. XV Beilage-Bd. 1902. + + \MERICAN GEOLOGIST, VOL. XXXI. PLaTE III. grthogoniacea Dorsal voavpiosorduhS Dorsal 5 > a) 0 re S SS rw ventral ventral ~ “BS 7) os “0, RS nee 0: Oro anal axis N : Growth axis nm - Anterior V - Posterior P : Pallia) sinus PIIPIUDSOINeIS Musele impression by ale Mehl } - en UUML THAN arr A fiw, dele iG ae ae rie Noetling on the Pelecypods.—Ruedemann. 35 of the hinge line as constant. Noetling holds that it would seem a priori possible that the valves or the hinge line should have, in different genera a different position in regard to the principal axes of the animal. He has eliminated the miscon- ception arising from the assumption of the stable position of the hinge line by considering the oro-anal axis of the animal as a constant line. But even this new conception would not furnish the clew to the law of torsion as long as the hinge line is considered (as by Jackson) one radius of the angle of tor- sion; with Noetling’s data a comparison of the valves of Nu- cula with any sinupalliate pelecypod valve shows, that though in both the axis of the hinge is parallel to the oro-anal axis, a torison of 90° of the valve of Nucula has taken place with ref- erence to that of the sinupalliates. The suggested law of torsion, however, can not be clearly conceived without a thorough understanding of the relations of hight and length of the shell. The investigation of this re- lation led to the cognition of the fact that the term “hight,” as conventionally derived by placing the shell in a vertical po- sition with the ligament forming the dorsal line, is an in- definite term, in many cases is not Jiomologous and in Pecten and Venus may represent very different axes. Noet- ling, therefore, defines “hight” and “leneth” by reference to- the oro-anal axis, viz. the length of the shell as the dis- tance between two points nearest the oral and anal-extremities and which are hence situated upon the oro-anal axis. With this dimension derived from the position of the animal within the shell the empirical “length” coincides, in the Dimyarians, but not in the Heteromyarians. In a shell of Pecten or Avic- ula we customarily measure the hight upon the oro-anal axis (See AO in diagram) and the so-called length upon a line connecting the dorsal and ventral margins. The terms have hence been simply inverted and it is evident that confusion herein cannot be avoided. In the Dimyaria (see Loxogoniacea of diagram) the length goes through both adductor muscles, in the Heteromyaria (Opisthogoniacea of diagram) the length passes between the two and in the Monomyaria (Symptogoniacea of diagram) the muscle has been so far removed from the oro-anal axis that a line, passing through the center of the former is perpen- dicular to the latter. 30 The American Geologist. TABU aT ee, Under “hight” one understands conventionally the greatest vertical distance between points of the dorsal and ventral mar- gins. Noetling shows, first, that the length of this line, thus defined, depends largely upon. the curvature and the thick- ness of the shell, which are accidental, indefinite elements. To eliminate these and because this “hight”? is not com- parable in Dimyaria and Heteromyaria, the author defines as the “true hight” the distance between the ventral margin and the ventral edge of the hinge-plate, measured upon a line, which is perpendicular to the oro-anal axis and passes through the mouth. For the mathematical expression of the torsion of the shell it has been found necessary to define a third element of the shell which is considered as of the greatest significance. For example, in the shell of Cypricardia, there is a ridge from umbo to ventro-posterior margin, the umbonal ridge (see dia- gram 1), which marks the direction of greatest longitudinal growth of the valve. This line is termed the “Crescenz-linie” (growth-axis). Its horizontal projection forms an angle with the oro-anal axis, which is termed the ‘“Schalenschiefe’” (ob- liquity or slant of shell). é H It can now be shown that the expression aa (an angle of obliquity) allows the mathematical determination of the Schalenschiefe. The possible values of « between o° and 360 give an infinite number of stages of torsion which the author chooses to place in 8 groups. In the determination of these groups it is to be remembered that not the shell, but the animal within the shell determines the terms applied to the parts of the shell, and that the oro-anal axis hes in the hori- zontal line, as it does during the life time of the animal. The groups are: I) a= 0° (or 360 ), that is, both axes (growth-axis and length or oro-anal axis) coincide. In this case the growth must take place in the direction of the oro-anal axis, and in a posterior direction. These are the Symptogomacea and as classical example for the group is cited Pecten, where growth takes place in an anal direction. The hight = o. 2) (eet. Or but < OO", tallie, > 0, ’ bit oO, but < 180, tan a < 1, but with different sign than case 2. i The two axes form an obtuse angle and growth takes place in antero-ventral direction; Prosogoniacea. ‘These correspond to the Loxogoniacea (see diagram) and a right valve of the Loxogoniacea is similar to a left valve of the Prosogoniacea. Mesodesma donacina and Nucula are mentioned as character- istic representatives and it is stated that in depending solely upon the external characters of the shell, one would consider the longer anterior part as the posterior one, as is done indeed in most descriptions. ee —" Poo. tan a= o> A’ =o. Amphigonacea. These correspond to the Symptogoniacea, both axes coincide again, but growth takes place in opposite direction, viz. forward. No examples are known to the author, but it is thought that they would have to be looked for among paleozoic forms, which might have the pallial sinus or the posterior muscle near the umbo. ine IO Shi << 270" :'tan a>. Oo, buti< 1; H.< L. Here the Schalenschiefe forms an angle in the third quad- rant and mathematically we have the case of the Loxogoniacea ; and upon the shell the two axes would form an acute angle, but in. fact the angle is greater than 2 R (R = right angle, see diagram), and growth takes place in dorso-oral direction, i.e. the ventral organs would lie below the umbo and the dorsal organs near the free shell margin. No examples of these, the Protoconchae, are known, and the author concedes that it will be difficult to find any; but adds that among such paleozoic Dimyaria as have an acute “Schalenschiefe” a pallial sinus near the umbo should be sought. Pip 270} tanes "1 3H = R: 38 The American Geologist. January, ane These, the Staurogoniacea, correspond mathematically to the Orthogoniacea, but growth takes place in an opposite di- rection, i.e. dorsally. No example known, but they are to be sought among the paleozoic forms with a rectangular “Scha- lenschiefe.”’ 8) 3270°, but <"360> tame '<- x, but >a; Eee Among these, the Opisthogonicea, the Schalenschiefe forms an angle in the fourth quadrant. As « = 3R+ @!, the Scha- lenschiefe forms again apparently an acute angle, but the growth takes place in dorso-anal direction. To this group belong the Heteromyaria and Avicula can be considered as its type. These are the eight cases, which, according to Noetling, are possible for the size of the Schalenschiefe. In four of these, where 4 =o0°, 1R, 2R, 3R the number of possibilities is absolutely limited but where «=o +41 (acute angle), IR+¢! (obtuse), 2R+a! (acute in third quadrant), 3R+' (acute in fourth quadrant), the number of possible sizes is indefinite. 4 appears therefore always as an acute angle and the great diffi- culty is to determine to which quadrant it belongs. Where the pallial sinus can ‘be observed no difficulty is found to determine whether « lies in the first or second quadrant; the external ligament can also be used for this purpose. The direction of growth of the shell will readily decide whether «@ lies in the fourth quadrant. If the shell in question covers none of these eases and a is acute it could be logically concluded that it lies in the third quadrant. As with paleozoic fossils both the ex- ternal ligaments and the pallial sinus often fail of observation, this determination will mostly be very difficult and other cri- teria are therefore sought for. The author has the eight cases under discussion, so ar- ranged in a diagram, that they form a closed circle. This diagram is here copied. All figures of valves are placed so that the dorsal side is above and the oro-anal axis (A-O) lies hori- zontal, W represents the axis of growth, the latter having tak- en place in the direction of the marker. The central ring of angles represents the corresponding Schalenschiefe, the angle formed by the axis of growth and the oro-anal axis. The torsion of the shells becomes in this diagram directly apparent. Mr. Noetling then points out the deep hiatus existing be- Noetling on the Pelecypods.—Ruedemann, 39 tween the Loxogoniacea (sinupalliate Dimyaria) and the Symptogoniacea (Monomyaria), which in this diagram have become adjoining groups; while each of them is in the other direction connected with the next adjoining group; the Symp- togoniacea being generally considered as derived from the Opisthogoniacea, and the Loxogoniacea being closely related to the Orthogoniacea. Altogether there seems to exist from the Loxogoniacea in a direction against the movement of the hands of the watch a continuous series of groups, and from the Symptogoniacea with the movement of the hands of the watch. This leads to the conclusion that the two, Loxogoniacea and Symptogoniacea, represent the termini of two series, which are thought to begin with the Protoconchae. In the diagram this supposed phylogenetic connection is indicated by the circle which beginning at the Protoconchae is, in the upper semi- circle, marked as the phylum of the Dimyaria, in the lower as that of the Monomyaria. The problematic group of the Protoconchae which would represent the primitive pelecypods, can be said to possess the following characters: Equivalve, but inequilateral. Two mus- cular impressions. Pallial line entire, without sinus, situated upon the umbonal side of the shell, i. e. with its convexity di- rected toward the umbo. Hinge consisting of primary lamel- lae. Ligament partly external, partly internal. Schalenschiefe between 180° and 270°, and growth in oro-dorsal direction. On the whole the shell would be like that of a common dimyarian, but the animal lay in it turned 180’, so that the ventral organs were situated in the umbonal direction. It is stated that this definition of the Protoconchae tallies in the more important features with that furnished by Dall in Zittel-Eastman’s text- book of the Protopelecypoda, and derived from the characters of the prodissoconch. The difficulty of recognizing this im- portant group among the paleozoic pelecypods is conceded, and it is added that only the pallial line and the direction of growth will definitely determine the existence of this group. The author thinks that these groups could be also used for systematic purposes, specially as several coincide in the whole, with classes of the original system of pelecypods. It would seem, however, to the writer that the groups can not be of equal value, as some represent only a single momentary stage 40 The American Geologist. pt in the process of torsion, in the Orthogoniacea for instance, that stage where the axis of growth has just become vertical upon the oro-anal axis (4 = 90), while the neighboring groups of the Prosogoniacea and Loxogoniacea each comprise an entire extent of torsion of 90°. This becomes also evident from the fact that while the Loxogoniacea are claimed to co- incide with most of the sinupalliate Dimyaria, under the Ortho- goniacea, it can be only said, that besides Pectunculus also Cardium shows in many cases a Schalenschiefe of 90. The Orthogoniacea would, hence, appear as only a limitary case of the Loxogoniacea. By applying the mathematical divisions in their full sharpness, the system would, it seems, become too rigid for the use of the biologist and some groups perhaps would be represented only by a few species of several differ- ent genera. In the final chapter of this paper, which it is hoped will inject new life in the difficult study of the paleozoic pele- cypods, and will perhaps dissolve the “Palaeoconchae” just as the long esteemed class of the Tetracoralla has been dis- solved, paleontologists are cautioned in regard to the use of the terminology, for, assuming the actuality of the torsion, it would be absurd to continue, in Pecten for example, the terms anterior and posterior ears, or to designate the posterior mar- gin as ventral margin, as has been done hitherto. In such groups as the Prosogoniacea the danger is even that right and left valves may be confounded. NOTE ON THE WEST INDIAN ERUPTIONS OF IIO2: (No true Lateral Ciaters took part in the Volcanic Eruptions.) By GEO. CARROLL CURTIs, Boston. The existence of lower active craters on the slopes of Pelée has been reported in connection with the recent eruptions,” but, after what up to the time of my departure, July 6th, had been the most complete field reconnoissance in St. Vincent and Martinique since the eruption, I am inclined to believe that no true lateral or parasitic lower craters of terrestrial origin have taken part in the eruption of 1902. * ANGELO HEILPRIN. McClure’s Mag., Aug., 1902. ROBERT T. HILL, Nat. Geog. Mag., vol. viii, No. 7. West Indian Eruptions of 1902.—Curtis. 41 It‘ is quite probable that within the great crater of Pelée there may be several vents besides the summit opening, in fact I observed three very distinct loci from which eruptions ap- peared to come within the walls of the main crater. From the very nature of the fragmental cone within, it is wholly con- sistent that volcanic outbursts may fissure it at various places along the flanks, and I am inclined to believe that outbreaks from the lower side of the great interior cone may have fre- quently been interpreted as eruptions from lower craters. These local manifestations in the main crater, however, no more deserve separation from the main source than would different puffs of smoke which emanate from the periphery of a bonfire. , A phenomenon which [ saw to cause much fright among the natives of both St. Vincent and Martinique, was eruption in the beds of rivers. This spectacular, though comparatively harmless expression, I am persuaded to believe is of wholly secondary nature, and of no more subterranean origin than is the cake of ice delivered at the door a source of winter rigor. The processes of these local eruptions could be seen by close, rational observation on the spot. At a distance they were misinterpreted by all except those who had learned their meaning from studies at close range. There are several im- mediate causes of these river bed eruptions and those methods by which I have observed them to be brought about. ~ While returning in a canoe on the afternoon of May 3rd from a trip along the northern shore of St. Vincent, there came on a heavy rain. In a few minutes the water was fairly washing down the land over the cliffs into the sea. Rills became small torrents and hanging drainage creases sent small niagaras black with ash mud down the steep cliffs. Then just opposite a great cloud sprang from the mouth of the Wallibou river, and with a startling roar the heavy clouds rose higher and higher in great convoluting, twisting masses, huge fingers of black earth shot up through the stream in spasms and melted back into the bulging rolls. The eruption column rose to a hight of over a mile, curtaining in our horizon, darkening the sky and raining upon us a snow-like coating of wet ash dust. For over an hour we forced our unwilling boatmen to 42 The American Geologist. pati hit hold us in this shower of ash. Next morning a new’ delta 14 x 4o feet had grown at the mouth of the Wallibou. This eruption was largely due to the swollen stream reaching a hot ash _ bed. On June 24th I witnessed the mud flow from Pelee and all the evidence I obtained from revisiting the field to the crater’s mouth indicates that this was due to the water sent to the ash beds in the Séche and Blanche direct by an eruption from the 3 miles distant crater. No other explanation can I make hold, and there is much to substantiate the view. Origin and Action of Ash Deposits. Hot ejected rock of varying size from the impalpable dust to boulders 21 x 50 feet have been distributed over the great- er portion of the slopes of Mt. Pelée and the Soufriere, but while they seldom average above a depth of four or five feet on the upper surface, concentrations of from 20 to 100 feet have taken place within the narrow river beds. I am inclined to believe that one important method of this canyon concentration has been during great outbursts when large volumes of water have been erupted together with the heated rocks and dust, and that these masses have rushed down the mountain sides in great avalanches, some reaching the sea direct, forming deltas and even islands, others being deposited as a flood plain within the canyon walls, where the heavier boulders, gravitating to the lower portion, the upper part of the mud flow serves as a blanket to retain the heat. On May sth the Guerin factory on Martinique was buried some 60 feet under such a flow. The ash retained, at the time of our de- parture from Martinique, July 6th, sufficient heat to cause heavy columns of vapor whenever the canyon became flooded. It is by the access of water, whether by collection in heavy rain, by stream damming process, or by direct eruption from the crater or otherwise that these hot ash beds give vent to the geyser-like eruptions, sending out great clouds of steam and mud, which give the impression of a primary volcanic eruption. This has led to the belief that true terrestrial craters exist on the lower slopes. This secondary phenomenon has been the most instructive of the recent West Indian eruptions. It lay spread out, literally smoking hot, exposed to the observation of West Indian Eruptions of 1902.—Curtis. 43 all who would visit, and it is in a careful study of these tangi- ble remains that the contributions may be made to geological science. Crater of 1812. On the north east side of the Soufriére crater at St. Vin- cent lies a small lateral crater of about ™% the diameter of La Soufriere. Current rumor has it that this lateral crater which, is reported to have been formed by the eruption of 1812, had played an active part in the present eruption, and that the nar- row wall between the two vents had been broken away. On June 7th with Dr. E. O. Hovey and a black guide, Samuel Brown of the destroyed Lot 14 Estate. I succeeded in reaching the crater of 1812 and crawled for some distance out upon the narrow divide which separates it from the great crater of “La Soufri¢re.’ The wall was still standing, no evidence that could be gathered indicated the small crater had been in eruption during the recent outbreak. The eruptions in Martinique have occurred within the somma ring of the great summit crater of Mt. Pelée which though divided into several foci of activity can scarcely be re- garded as possessing lateral vents. From this I believe that while manifestations of volcanic energy in the form of outbursts of dust laden steam within the river beds have been frequently observed, no true lateral vol- canic eruptions have taken place and no true lateral or para- sitic craters have yet been formed in the West Indian eruption of 1902. MINERALS OBSERVED ON BURIED CHINESE COINS: OF THE (SEVENTH CENTURY. By AUSTIN F. ROGERS, New York. Anything that throws light on the formation of minerals is welcome to the mineralogist, geologist and student of ore deposits. © Principal among the objects furnishing such light are the so-called artificial minerals, products of the laboratory and furnace. There is another class of objects forming, as it were, a con- necting link between minerals and artificial minerals which 44 The American Geologist. ane aid us in studying the formation of minerals. I refer to min- erals found on timbers and tools in abandoned mines, on metal- lic utensils buried for vears, on slags exposed to the elements and the like. In these there is an element of the artificial. Man has accidentally placed the objects which are acted upon in certain favorable places but has not directed the conditions of the experiments. In this connection we recall Daubrée’s clas- sic researches on the minerals found in the Roman baths at the thermal springs of Plombieres. But it is minerals formed upon and at the expense of buried coins that I wish to consider now. The coins heretofore de- scribed are Roman coins, found in France, Algeria, Corsica, and England. Four out of the five minerals observed on our Chinese coins have been observed on these Roman coins. In grading the grounds of the William Nast College (for Chinese) at Kiukiang, China, a pot of buried coins was discoy- ered. The pot contained about five thousand copper coins. They were brought to this country by bishop David H. Moore of the Methodist Episcopal church, and one of them is given as a souvenir receipt to everyone who subscribes a dollar toward the fund for a college dormitory. No facts regarding the oc- currence of the coins were obtainable. They are the circular “cash: ‘with a*square hole in the-center. (On Some jotutiiem the inscription is well preserved and, according to the printed slip accompanying them, the coinage is of the Kang dynasty, Kai Yuan reign, seventh century. The writer had the oppor- tunity of looking over several hundred coins in the possession of bishop Moore, to whom he wishes to express his thanks. As a rule the coins are not much corroded. On many the inscrip- tions are plain and a few strokes of the file usually reveals the bright metal of the coin which is largely copper. The minerals observed are cuprite, malachite, azurite, copper, and cerussite. Many of the coins have little, if any, of these min- erals while others are almost completely covered on both sides. Some have only one or two of the minerals while others have three or four or in one case five. On one coin, one mineral may be dominant, on another it may be a different mineral. Though some of the coins have cuprite on one side and the copper carbonates on the other there is no regularity of such distribution. In the case of three of the copper minerals, there Buried Chinese Coins.—Roegers. 45 Z 5 is a definite order of succession.—The cuprite was formed first, then the malachite, then the azurite. Nearly all the specimens exhibit this paragenesis. Cuprite—Cuprite usually occurs in small but distinct crys- tals. When the crystals with their brilliant reflecting surfaces are thickly scattered over the surface the coin makes a beautiful specimen. The dominant crystal forms are the cube and the octahedron. There are also the dodecahedron, a trapezohedron and a tetrahexahedron. On the best specimen the crystals pre- sent the following combination: cube, dodecahedron, octahe- dron and a trapezohedron. Several crystals were measured and the first three forms identified, but no indices could be as- signed to the trapezohedron. On other coins octahedral crys- tals occur. Malachite——A mammillated structure with concentric lay- ers characterizes the malachite. It has been formed after the cuprite and before the azurite. Azurite.—Azurite does not occur as often or in as large amounts as malachite. It is often crystalline in structure, its drusy surface following the contour of the malachite, the formation of which preceded it. Copper.—Small, rough crystals of copper were observ a on two of the coins associated with cuprite. Cerussite—Cerussite was found on nearly all the coins ex- amined. Though usually in subordinate amount, on one coin it was the dominant mineral. It is sometimes colored with cuprite. The lead probably came from some extraneous source as none could be detected in the coin itself. With the exception of the copper our occurrence is like that noted by Fletcher* on Roman coins from Chester. Appended is a list of minerals that have been found on coins with the names of observers, localities and references to publication. Azurite.—Lacroix—Algeria. Bull. soc. fr. Min. 6:175, 1883. Fletcher—Chester. Min. Mag., 7: 187, 1887. Bornite.—Daubrée— Bourboune les Bains. C. R. 80: 461,1875. Gouvenain—Bourbon l’Archambault. C. R. 80: 1297, 1875. Cerussite—Lacroix—Algeria. ibid. Fletcher—Chester. ibid. * Woe cit, 46 The American Geologist. Fanner yes Chalcocite—Daubrée—Bourbonne les Bains, ibid. Daubrée—Baracci, Corsica. C. R. 92: 57, 1881. Daubrée—Flines les Roches. C. R. 93:572, 1881. Chalcopyrite —Daubrée—Begneéres de Bigorre. Bull Soc. Geol. France 19: 529, 1862. Bourbonne les Bains. ibid. Flines les Roches. ibid. Daubrée Daubrée Gouvenain—Bourbon l’Archambault. ibid. Cuprite.—Fletcher—Chester. ibid. Breislak—Torre del Greco. Physische u. lithologische Reisen durch Campanien, 1802, p. 204. Malachite—Lacroix—Algeria. ibid. Fletcher—Chester. ibid. Tetrahedrite—Daubrée—Bourbonne les Bains. ibid. Columbia University in the city of New York, Dec., 1¢02. AN ERRATIC BOWLDER FROM THE COAL MEASURES OF TENNESSEE. By S. W. McCaLttk, Asst. Geologist of Georgia, Atlanta. Two vears ago last summer while on a visit to the Etna coal mines located near Chattanooga, Tenn., my attention was called to a bowlder which a short time before had been found near the center of a three-foot coal seam. The main attractive feature of the bowlder to the miners, and apparently the cause which led to its preservation from the waste dump, seemed to have been the glittering particles of pyrite to be seen at several points on its surface. The pyrite was supposed by the miners to be gold, and as a consequence the bowlder was spoken of as the “gold rock.” The writer learned that a short time previous to his visit, the bowlder had been shown to one of the United States geol- ogists, who, though then engaged in collecting fossil coal plants at the mines, broke off and carried away a small piece of the stone. With the exception of the removal of this fragment and a few marks made by the pick in dislodging it from the coal seam, the bowlder was entire and not otherwise mutilated. The bowlder was elongated, somewhat kidney-shaped, and would weigh when entire twenty or thirty pounds. Its sur- face was quite smooth and had every appearance of having been water worn. In shape and in size it was not at all unlike An Erratic Bowlder.—McCallie. 47 stones frequently met with in or near the larger streams of East Tennessee and North Georgia, but on close examination it was found to be entirely different both in structure and min- eralogical composition. The color of the stone is greenish gray, specked with small, irregular dark and light colored spots. In texture it is fine- grained, none of the individual minerals being made out ma- croscopically. Thin sections show that it consists of quartz and feldspar phenocrysts and biotite, in a quartz-feldspar ‘ground mass. The feldspar and also the biotite are usually much altered, the former giving rise to scales of kaolin, and the latter to chlorite. Whether these alterations antedate the burial of the rock in the Coal Measures, or are of subsequent date, is an open question. However, the smooth surface of the bowlder would seem to indicate that the stone was polished by water when che minerals were in a comparatively fresh state. A specimen of the rock submitted to Miss Florence Bas- com, of Bryn Mawr, for examination was identified by her as an aporhyolyte, though she suggested that the more general term metarhyolyte might also be used. Miss Bascom was un- able to decide definitely from a single slide whether the rock cooled as a lava flow, or as a dike, yet no doubt was expressed as to its classification. The most interesting question which suggests itself in re- gard to this erratic bowlder is its source. Its water-worn surface would seem to indicate that 1t had probably been trans- ported some clistance by water prior to its deposition in the coal seam, but even this throws littla or no light on its original source, as no rocks of like character are to be found in Tennes- see or the adjacent portions of Georgia and Alabama. The stratigraphical position of the bowlder fixes the time of its deposition in the latter half of the Carboniferous age, and as a consequence the lava flow or dike from which the bowlder was derived must antedate that period. This would seem to indi- cate that prior to the latter half of the Carboniferous age at some point not far removed from the Etna coal mines there were dikes or surface flows of rhyolyte which have since been buried beneath subsequent deposits. 48 The American Geologist. ‘SO6T ‘Aaenuer GEOLOGICAL AGE OF THE WEST INDIAN VOL- CANIC FORMATIONS. By J. W. SPENCER, Toronto. The Greater Antilles appear to be nearly devoid of volcan- oes. The writer has seen only the remains of one in Jamaica (at Low Layton), and none in Cuba. But there are extensive underlying igneous formations in all these islands. How- ever, in the inner zone of the Caribbean or Windward islands there are many cones, and beneath these and the outer islands there is an underlying volcanic basement. In such of the outer islands as St. Martin and better still in Antigua, and in St. Croix one gets some knowledge of the antiquity of the older eruptive formations. In Guadeloupe the geological records are equally well preserved, on one side, while on the other there are the more recent volcanic cones, which can also be seen in St. Kitts, Statia, Dominiqua, Martinique, St. Lucia, St. Vincent, etc. : ——Bank e & a =p Calon Bi ¢ ew og Ss OF ; c 3 ae S es ay 2, teh ee Sombrero a °° Supa oe’ FO we X Meee oSyangala fone wake Z a I ob, S'S Afaron pane Sta Cran? Sabal, S = /StBaxtholenew neo cSabda. So eee: ree see af 6 Montserrat Guadeloupe \ { Avesl NEY eee g StaLucia % Sc¥incent Ys Barbados cArcona Breakers ive i (fe. GRENADINES c ae Aims scou ” In St. Martin and Antiqua the old volcanic basement forms mountains still uncovered by modern cones, as also in St. Xe pt West Indian Volcanic Formations.—S pencer. 49 Croix. The rocks are essentially an andesyte in form of both lavas and tuffs. Their surface topography is moulded by at- mospheric agents into low mountains and valleys. Overlying such a basement in St. Croix and St. Thomas, according to Cleve,* there is a conglomerate containing pebbles with Cre- taceous fossils. In this region these basement rocks are so dissected that their remains constitute many of the islands of the Virgin group. But in Antigua and Grande Terre of Guadeloupe the strata overlying the denuded igneous basement isasub-aqueous re-distributed tuff with some calcareous beds in the upper zone, over which rest conformably the white limestones, a marly deposit containing Oligocene corals and shells.+ South of the Guadeloupe archipelago and Monserrat, the outer islands dis- ‘appear, and the writer is not aware of the occurrence of the early Tertiary limestones remaining so as to leave evidence of the age of the igneous basement, though by its lithological ‘characteristics and the physical features of its ancient surface one can hardly be far astray in concluding that they are of the same age as the similar formations on the islands to the north. In Barbados the Oligocene limestones reappear, but here there are no igneous deposits. It thus seems that the whole Carib- bean plateau beneath both the volcanic ridges and the lime- stone islands is underlaid by an igneous formation dating back to the commencement of the Tertiary period at least, if indeed these rocks are not as old as those of St. Croix, that is as an- cient as the Cretaceous period. In St. Martin, St. Bartholomew and Antigua, the moun- tain belts are entirely made up of the denuded rocks of this old igneous formation without a covering mantle. So also, part of Statia, St. Kitts, Monserrat, the southern end of Mar- tinique, portions of St. Lucia and the southern end St. Vincent have their surfaces moulded out of the ancient igneous accum- ulations; but elsewhere in these islands, as also in Guadeloupe proper and Dominique, they are covered with volcanic mater- ials which constitute more or less of the cones and ridges ris- ing to a hight of 3,000 to 4,000 feet. In these mountainous * On the Geology of the northeastern West Indian islands. Trans. Roy. Sociedad Acad. Sci., vol. ix. 1870-71. +See “Geological and Physical Development’’ of the various Windward islands, in six papers by J. W. SPENCER, in Quart. Jour. Geol, Sci., vol. ivil (1901), pp. 409-543, and vol. lviii, (1902), pp. 341-365. 50 The American Geologist. Janda | eee islands, there is not merely a combination of late and ancient eruptive deposits, but there are several formations secondarily derived from the remains of the older basement, and here is room for more study than has been attempted. The history of one is more or less the history of all these conical islands. For instance, in Dominique there is the old andesitic rock overlaid by volcanic breccia or conglomerate. At other points the age of the tuffs cannot at present be as- signed, but some of them have been denuded into relatively large valleys which have been partly refilled with still newer tuffs (like that of the Roseau valley) containing an abundance of water-worn pebbles, often arranged in lines among the more angular material. Such may correspond to the early Tertiary sub-aqueous tufaceous beds of Grand Terre (Guadeloupe). And these beds have been subsequently tilted outwards at considerable angles. As in St. Martin, Antigua and Grand Terre, there is nothing to show that there were any mid-Ter- tiary eruptions when the whole region was somewhat elevated and the denuding agents were moulding the surface into rounded outlines. From the corresponding topography in the more volcanic islands, where not surmounted by the modern cones, the impression is left that the volcanic activity of the region was quiescent during much of the Miocene-Pliocene period, before the building up of the cones and ridges; which were constructed at a relatively late date; for we find the sea- bed elevated along with these ridges. Thus we find in Statia and in St. Kitts volcanic cones raised by an upward thrust which carried along with it the sea-floor covered by about 30 feet of marl, now forming broken mantles surrounding the cones to elevations of from 400 to goo feet. Elsewhere, how- ever, we find fragments of a similar formation appearing with the volcanic rocks brought up by a general elevation of the is- land. These limestone marls contain practically a living fauna, thus showing the elevation to date no farther back than the end of the Pliocene period. Again there are two series of gravel formations, one of which is older than the coralline strata just mentioned as interbedded with the volcanic ejectamenta; but this gravel formation had its surface greatly denuded before the formation of the marl. Again, both the marl and the gravel have been further subjected to erosion so as to often be only West Indian Volcanic Formations.—S pencer. 51 left in broken series. The newer gravel has not been sub- jected to so much denudation. The youthful lavas have been seen both in Dominigua and St. Kitts, beneath the stratified gravel beds at present not determined as to whether belonging to the older or newer series. The lower gravels in their succession correspond in position to the Lafayette of the con- tinent, and the upper gravels to that of the Columbia. The eruption which raised the cones in St. Kitts and Statia, above referred to, appears to have occurred during the subsidence which gave rise to the upper gravels provisionally regarded as the equivalent of the Columbian series,—a mid-Pleistocene formation—and the marl beds thus raised rest upon an inco- herent bed of volcanic ashes, containing living fauna. From all facts before the writer it seems that the volcanic ridges owe their origin to volcanic activity which re-commenced about the close of the Pliocene period, and that the eruptions have continued with more or less interruption down to the present day, for we find that the cones and ridges have not become so deeply dissected by rains and streams as would be expected had their growth not been continued more or less continu- ously from their re-birth at the close of the Pliocene period to the present year of recorded activity. EDITORIAL COMMENT. THE DIAMOND MINES OF SOUTH AFRICA. Just how much of the popular interest in diamonds is due to their value and beauty for personal adornment and how much to the difficulties in the way of satisfactorily accounting for their origin, it is perhaps impossible to say. The true sci- entist would, undoubtedly, claim that with him the latter in- terests were paramount. Still, there exists in our minds a doubt if, were diamonds as cheap and abundant as quartz crystals, the interest, even of these, would be as intense. Be this as it may, from the earliest period when stones of high refractive index were faceted, the diamond and all relat- ing thereto has possessed a fascination for the general reader beyond that of all other gems. A recent work, ‘““The Diamond Mines of South Africa’ by Gardner F. Williams (The Mac- 2 The American Geologist. aah). on millan Co., 1902), adds one more to a long list of titles and presents the subject, so far as South Africa, at least, is con- cerned, in a manner never yet equaled for attractiveness and thoroughness. The work comprises 681 royal octavo pages, with 29 photogravure plates, 11 maps, and nearly 500 figures in the text. There is space here, certainly, for a satisfactory review of the subject, and it has been, apparently, well utilized. Numerous references to other writers and the fact that the writer is general manager of the De Beers Consolidated Mines tend to give the work an air of authority which it might not otherwise possess. The book begins with an account of the ancient Adamas, the references to the diamond in early scriptural and profane literature, a chapter on the traditional Ophir Land, including a history of the various settlements in South Africa and the final crowding out of the Boers from the Cane Colony by the British and their trekking into the Transvaal. The stories of the experiences of these hardy emigrants and their conflicts with the natives read almost like the early histories of the western emigrants in our own country. The matter of the early discovery of the diamond is taken up in considerable detail and the account which the writer seems to regard as most authentic is the one which has here- tofore often found its way into print. It tells of the finding by a farmer’s child of one little white stone, which was carried home and left carelessly lying about upon the floor until dis- covered by a neighbor, Schalk van Niekerk, to whom it was given by the mother of the child, and who subsequently placed it in the hands of a traveling trader, John O’Reilly. From O’Reilly it passed into the keeping of the acting Civil Com- missioner at Colesberg, Mr. Lorenzo Boyes, and then to Dr. Atherstone at Grahamstown, by whom it was finally identified as a diamond. This finding, however, failed to create any great sensation, and it was nearly ten months later that a second one was found, and this at a point some thirty miles distant. In March, 1869, a superb white diamond weighing 83% carats was picked up by a Griqua shepherd boy at Zendfontein near the Orange river. This also passed into the hands of Schalk van Niekerk, who paid for it five hundred sheep, ten oxen, and a horse, and subsequently sold it for £11,200 to Lil- Editorial Comment. 53 ienfeld Bros. of Hopetown. This stone was finally purchased by the Earl Dudley for £25,000, and was apparently the stone which first made the South African fields famous. A graphic account is given of the motley throng of for- tune hunters who poured into the region after the boom was fairly established and the confusion of titles which arose through conflicting mining claims. Details are also given of the manner in which the mines passed from the control of the Dutch and the native tribes into the hands of the English. The history of the development of the various mining claims and the final consolidation through the work of Cecil Rhodes and the young Hebrew, Barnett Isaacs, or Barney Barnato, as he was called, is given in considerable detail. Abundant illustra- tions show all the details of mining and various stages of de- velopment, and much that is incidental thereto. What is the least satisfactory chapter in the book, to the scientific man, at least, is that relating to the genesis of the diamond. Here no reference is made to the work of Daubree or De Launay, though the work of Carvill, Lewis, W. Luzi, and Rutley is quoted. The closing chapter, “An Uplifting Power,” has to do with the development of South Africa through the discovery of the diamond mines, and an appendix with the condition of the mines during the South African war. It would require no reference to the title page to assure the reader that both the latter were written by an Englishman and from an English- man’s standpoint, by one who was perhaps too near the scene of action and too closely connected by ties of blood to look at matters from a wholly impartial standpoint. G. P. M. REVIEW OF RECENT GEOLOGICAL LITERATURE. Om Slarpsbackens Dalgang, af John Chr., Moberg (Aftryck ur geol. foren. i-Stockholm forhandl., Bd. 24, H. 5, 1902.) This is a description of the vale of Sularp showing the outcrops of the several beds of shale with various species of graptolites, that are found along its course. The shales are Ordovician throughout. A map of the valley, showing the various features of interest along its course, accompanies the paper. GF M: 54 The American Geologist. Janae A Contribution to the Petrography of the John Day Basin. By FRANK C. Catxins. (Bull. Dept. Geol. of the University of California, Aug., 1902, vol. 3, No. 5.) The John Day Basin has yielded such important contributions to vertebrate paleontology that its history is of unusual’ interest. This paper shows the region in a new light, namely that of an important petrographic province. Since the beginning of Cretaceous time the region has been de- fined as a basin of accumulation, conditions of sedimentation alternat- ing with volcanic eruptions. It has suffered frequent crustal disturb- ance, and has been subjected to more or less erosion both in, recent time and in various intervals between volcanic outbursts. The mate- rial appears to be largely of pyroclastic origin. Considered as a petrographic province, the John Day basin seems to be characterized by the fact that its rocks are derived from gab- bro-peridotyte and granito-dioryte magmas, with an entire absence of rocks of the nepheline group. The analyses show a preponderance of soda molecules over potash and a recurrence of anorthoclase-bearing rhyolytes in Eocene, Miocene and Pliocene times. The order of successior, of types affords a fairly strong confirm- ation of Iddings’s theory that the normal succession is from intermedi- ate to more basic and more acid types. In the Eocene there was a complete cycle of this kind: in the Miocene and Pliocene a second: a recent ash represents the beginning of a third cycle. The great preponderaace of pyroclastic material indicates that these beds were mainly of terrestrial origin, and affords further evidence in favor of the theory of Matthew and disproof of the lacustrine or- igin of these beds. We 80s (Oy Maryland Geological Survey, Volume IV. W. Buttock Crark. Since the organizatior, of the Maryland Geological Survey in the spring of 1896 four volumes of the general reports have been issued and three volumes of special reports. The present volume, the fourth in the series of general reports, possesses the same high degree of practical and scientific excellence which has characterized the other publications of the Survey. A discussion of Paleozoic Appalachia or the History of Maryland during Paleozoic Time by Bailey Willis constitutes Part I. of the vol- ume, and comprises the geologic history of eastern North America from the pre-Cambrian time to the present. The paper opens with a discussion of the geologic processes which make geologic history and proceeds with an account of the development and wasting of Appalachia, the advance and retreat of the Mediterran- ean sea of North America, the growth of Paleozoic coastal plains, the accumulation, dislocation and folding of Paleozoic sediments, and the formation of post-Paleozoic peneplains. This exposition possesses the rare value, which the author’s perfect familiarity with the great multiplicity of facts presented by the Appal- Review of Recent Geological Literature. 55 achian field, his experimental mastery of the dynamics of rock move- ment, his ability to draw broad generalizations and his unusual lucidity of statement, are able to give to it. The paper presents an invaluable reading lesson for college students of historical geology. Part II. contains The Second Report on the Highways of Maryland by Harry Fielding Reid ard A. N. Jolson. The first report present- ed the condition of the highways throughout the state and outlined methods of improved road making. The present report gives an account of the work which has deen conducted under the supervision of the Highway Division of the Mary- land Geological Survey: It describes some new methods of testing road material which have beer, devised in the laboratory of the Divis- jon, and closes with a report of the Baltimore County Roads Engineer. The report makes very clear the important fact that the highways of Maryland can be permanently improved by the intelligent use of means now available in the state without additional cost. The work of this division of the Survey is plainly of immediate practical value to the state. Part III. comprises a Report on the Clays of Maryland by Hein- rich Ries. The report opens with an elaborate discussion of the cr- igin, properties and uses of clays with special reference to those of Maryland. Dr. Ries also discusses methods of testing clays ard shows how qualities: injurious to the clay for commercial purposes can be counteracted by the addition of proper ingredients. The second part of the report deals with the geologic distribution ard character of the Maryland clays and their relation to transpor- tation facilities. Maryland ranks eleventh in the list of clay producing states and seventh as a producer of pottery and yet possesses a very large unutil- ized supply of plastic material. It is the aim of this part of the re- port to bring to public knowledge the distribution and character of this unutilized material. A bibliography of accessible publications on, clay and a directory of Maryland clay workers are appended. This exhaustive report on Maryland’s clay wealth by an expert in the subject must possess great interest for the practical operator. All the reports are well and fully illustrated by maps, cuts and photo- graphs. F. B. Les roches volcaniques de la Martinique. A. Lacrorx (Comptes Rendus. May. 1902.). Prof. Lacroix here recalls descriptions of the rocks of Martinique published by himself in the Comptes Rendus in 1890. They were specimens of the collection of Ch. Sainte-Claire Deville preserved in the College de France at Paris, He showed that the presence of hypersthene in the volcanic rocks of Martinique and of Guadeloupe is an essential and almost constant character. “The earlier volcanic rocks are divided into three groups: dacytes, andesytes and labradorytes. They form dykes, flows and conglomer- ates accompanied by beds of ash. 1 G The American Geologist. January aie “Dacytes. The medium type of these rocks presents the greatest. analogy, in outer aspect, with the esterellyte of San Raphael. With the naked eye can be distinguished large crystals of quartz with double terminations, hornblende biotite, hypersthene and plagioclase scattered in a microcrystalline paste of a bluish gray color.. The rocks of Grand Piton, of the rocky Piton of Morne near Macouba, afford good ex- amples. “With the microscope it can be seen that the hornblende and the biotite are in course of resorption, the feldspars are much zoned, gen- erally with the central part most basic, but often also with a succession of zones alternating of two different feldspars. These feldspars are nearly always flattened parallel to g*, with a combination of Carlsbad, albite and pericline twinning. Their determination is therefore quite easy. The most common types are labradorite with 60 per cent of an- orthite, and andesine. Vitreous inclusions with bubbles are abundant, as in all the other volcanic rocks of Martinique. All these phenocrysts have a great tendency to unite together and form small segregations. The hornblende crystals are frequently ophitic with the feldspars. “The paste of the rock is constituted essentially of very small feld- pathic microlites, often themselves zoned, andesine and oligoclase. They are accompanied by quartz, sometimes granular, sumetimes poecilitic: frequently there exists numerous microlites and crystallites of hypers- thene. A considerable amount of titanic magnetite is seen sometimes in the microlites and sometimes in the phenocrysts. “Andesytes with hypersthene. The petrographic type which appears to be the most widely extended consists of acid andesytes of a light color, often having a porous or scoriaceous paste, rough to the touch, but which, in certain cases, is more compact and acquires a dark color in consequence of the abundance of vitreous matter. These rocks are andesytes with hypersthene in which the rhombic pyroxene is some- times accompanied by a little augite. The phenocrysts are, basides, formed of plagioclase of the andesine group. They are much zoned, but much less than in the labradorites. All these crystals are dissemin- ated in a glassy material which is more or less abundant, the feldspar microlites of which give extinctions that are sometimes longitudinal and sometimes oblique, only rarely reaching twenty degrees. (Carbet Laillet river, west. flank of Mont Pelée, environs’ of St. Pierre, of Precheur etc. ). “In several localities the glassy matter is replaced in part by globu- lar quartz sponges, the secondary character of which does not appear doubtful. (Upper valley of Pirogues, summit of Morne Jacob, etc.) “Hypersthene labradorytes. These rocks are distinguished, generally by the naked eye, from the andesytes by their doleritic aspect; they are usually of a dark gray color and more or less compact. Under the mi- croscope it can be seen, further, that the hypersthene is often sur- rounded by the augite with their axes parallel. Finally, sometimes olivine is apparent. The plagioclases are more zoned than in the pre- Review of Recent Geological Literature. 57 ‘ceding rocks. These very regular zones indicate considerable variation in composition which it is easy to individualize by reason of the almost constant presence of Carlsbad and albite twinning. One crystal ob- served, presented in its periphyry zone, perpendicular to the bisectrix Ng extinctions of 24° (labradorite with 55 per cent of anorthite) and at the centre an extinction of 51°, and the latter ought therefore to be classed with almost pure anorthite. “The microlites are themselves more basic, and exceed 20°, They are often accompanied by microlites of augite and of hypersthene. The study of a large number of specimens from the vicinity of Macouba, from the rivers Laillet, La Garde, and of blocks obtained in the con- glomerates of the same regions, causes me to believe that there exists a continuous series between these andesytes and these labradorytes. “Certain ones of the labradorytes contain ti> augite, but are rich in phenocrysts of ophitic hornblende. A homogeneous inclusion shows itself to be constituted of a basic dioryte (labrador-bytownite, horn- blende, hypersthene, augite) which ought to be considered as a deep- seated form of the labradorytes. “Augitic labradorytes. In conclusion there is reason to cite several rocks having a basaltic facies which are augitic labradorytes, with or without phenocrysts of basic plagioclase and of olivine. These are with- out phenocrysts of pyroxene (Fort de France). “The above summary description shows that the volcanic rocks of Martinique constitute a petrographic series remarkably distinct, com- prising rocks with free quartz (dacytes), rocks without quartz which by order of their increasing basicity are andesytes and labradorytes. Their common characteristic is their common essential element, a rhombic pyroxene, accompanied frequently by augite and by hornblende. The whole series is remarkable for the abundance of plagioclase phenocrysts. These are rarely homogeneous, but present the most beautiful examples that could be imagined of regular zones formed of differing composition. “To which of these petrographic types is it necessary to refer the products ejected to-day by Mont Pelée? We have as yet very little in- formation on this point. Nevertheless the ashes that fell on the night ‘of the 3d and 4th of May, the only ones that as yet we possess, de- scribed by Michel Levy at a previous meeting, have a mineralogic com- position which approaches the hypersthene andesytes described above. -They are very similar to a specimen of the collection of the Museum from the eruption of August 5th, 1851, and obtained in the form of a coating on a tree. Yet another specimen, of coarser ash, of I85I, is rich in fragments of hornblende. (May 26, 1902.)” In a later contribution to Martinique (June 2, 1902) Prof. Lacroix has instituted a comparison between the ash of Mont Pelée of 1851, and ‘the ash of the present eruption, and states that they differ very little, being very similar also to the ejecta of Mt. Shasta, in California, as de- termined by Hague and Iddings. They are hypersthene andesytes, no- tably less acid than those of Santorin (1866) or of Krakatoa, richer in alkalies, and poorer in alumina, magnesia and in lime. N. H. W. 58 The American Geologist. January, ees Structural Details in the Green Mountain Region and in Eastern New York. By. T. Netson Date. Bulletin of the United States Geo- logical Survey, No. 195. This is the second paper published by Mr. Dale under this title; the first paper appeared in the Sixteenth Annual Report of the U. S. Geol. Survey. (Pt. I., 1806, pp. 549-570.) Like the first publication the second is not a systematic exposition of the geology of the dis- tricts named, but a discussion of geologic details collected in the course of the exploration and mapping of seven U. S. Geological Sur- vey sheets. These are the Castleton, Pawlet, Equinox and Ben- nington sheets in western Vermont. The Greylock sheet of north- western Massachussetts and the Berlin and Tracy sheets in north- eastern New York. The formations underlain by Pre-Cambrian gneiss, include the sed- imentary series of the Algonkian, Cambrian and Ordovician—schists, quartzytes, slates, marbles, limestone and dolomytes. The intense dy- namic action to which they have been subjected has given rise to both open and close folding and in some cases, to faulting and shearing. As an exceptional occurrence, however, a recumbent isocline is de- scribed at Dorset, Vt., on the Pawlet sheet, a little southwest of Green Peak. Here also is shown a tendency to pinched folding which is more fully developed to the north on the Castleton sheet, at Pittsford. Some of the folds have suffered elongation so that the beds are thinned along the limbs and thickened at the crest. Perhaps the most noticeable feature of this locality is an over- thrust fault which begins at Pittsford and extends south for about ten miles to the town of Clarendon. The tangential force has been of sufficient intensity to produce a thrust fault whose strike is nearly north and south. The relation of the faulted beds is well shown on Boardman Hill north of Clarendon where Cambrian quartzyte on the east side of the fault is in contact with Upper Ordovician schists of the west side. There are two excellent plates which show how the over- turned major folds of the Cambrian quartzyte are plicated by minor folds. In Arlington at Roaring Brook on the Bennington sheet, shear- ing accompanies folding. The shear is indicated by borings of the Scolithus which were originally perpendicular to the bedding but are now deflected many degrees from verticality, The remainder of the paper is for the most part devoted to the discussion of the lithologic character of some of the formations, as well as to their structural relations. The Vermont marble is not a pure crystalline limestone, but is made up of coarse grained calcite marble interbedded with a fine grained rock which, by chemical anal- ysis, was proved to be a dolomyte.. Since both marble and dolomyte have undergone the same pressure, the difference in grain must be due, either to a difference in their behavior under pressure or to a difference in the original sediments. The Ordovician schists of the region are more interesting; the constituents are muscovite, quartz, chlorite, magnetite and albite feldspar with which are associated Review of Recent Geological Literature. 59 graphitic streaks parallel to the bedding. Shearing has also produced in the rock, a slip cleavage at right angles to the bedding. The rock is defined as a feldspar schist developed from a sediment. The pres- ence of albite places the formation among the gneisses. It is not un- like much of the schistose mica-gneiss of the Piedmont plateau. The paper closes with a discussion of the doubtful! conformity of the Cambrian rocks on the Pre-Cambrian gneiss. Good contacts are few but three are cited in the Green mountains where there is an evident unconformity in the strike of the rocks, As yet the discrep- ancy has not been explained which exists between these localities and others on Hoosac mountain, where the contact is conformable. Fur- ther study of this and other regions is necessary io harmonize these observations. ie MONTHLY AUTHOR’S CATALOGUE OF AMERICAN GEOLOGICAL LITERATURE ARRANGED ALPHABETICALLY. BARLOW, A. E. Dr. Alfred R. C. Selwyn, C.M.G., F.R.S., Director Geological Survey of Canada, 1869-1894, (Ott. Nat., vol. 16, pp. 171-177, Dec. 1902,. portrait.) BARBOUR, E. H. ( AND C. A. FISHER). New form of calcite-sand crystals. (Am. Jour. Sci., vol. 14. Dec. 1902. pp. 451-454.) BARTON, GEO. H. William Harmon Niles. (Tech. Review, vol. 4, 1902. portrait.) BAUER, L. A. United States magnetic declination tables and isogonic charts for 1902. Principal facts relating to the Earth’s magnetism. U. S. Coast and Geol. Sur. 1902. BEEDE, J. W. New fossils from the upnver Carboniferous of Kansas. (Kans. Univ. Sci. Bull., vol. 1, Sep. 1902. pp. 147-151.) BEEDE, J. W. Variation of the spiralia in Seminula argentia (Shepard) Hall. (Kans. Univ. Sci. Bull., vol. 1, Sept., 1902. pp. 155-157) BEEDE, J: W. Coal Measures faunal studies. II, Fauna of the Shawnee for- mation (Haworth), the Wabaunsee formation (Prosser), and the Cottonwood limestone. (Kans. Univ. Sci. Bull., vol. 1, pp. 163-181. Sept. 1902.) BROOKS, A. H. Preliminary report of the Ketchikan mining district. U.S. G. &. Prof. Pap. No. 1, pp. 120, 1902. 60 The American Geologist. JanUany ee BROWN, R. M. Clays of the Boston basin. (Am. Jour. Sci. vol. 14, Dec. 1902. pp. 445-450.) CALVIN, S. Concrete examples from the topography of Howard county, Iowa. (Am. Geol., vol. 30. pp. 375-381.) COLEMAN; A. P. Rock basins of Helen mine. Michipicoten, Canada. (Bull. GS: A., vol. 13. pp. 298-304, Oct., 1902.) : CONDRA, G. E. New Bryozoa from the Coal Measures of Nebraska. (Am. Geol., vol. 30. pp. 387-358, Dec. 1902.) : DALL, W. H. The Grand Gulf formation. (Sci. vol. 16, Dec. 12, 1902. p. 946.) EMERSON, J. S. Some characteristics of Kau. (Am. Jour. Sci., vol. 14, Dee. 1902. pp. 431-439.) F : FINLAY, GEO. I. Teneous rocks of the Algonkian series. (Bull. G. S. A., vol. 13. pp. 349-352.) FISHER, C. A. (E. H. BARBOUR AND). New form of calcite-sand crystals. (Am. Jour. Sci., vol. 14. Dec. 1902. pp. 451-454.) FOERSTE., A. F. The Cincinnati anticline in southern Kentucky. (Am. Geol., vol. 20. Dec. 1902, pp. 359-369.) FORD, W. E. Chemical composition of dumortierite. (Am. Jour. Sci., vol. 14, Dec. 1902, pp. 426-430.) FULLER, M. L. The Gaines oil field. (U.S.G.S., 22 Am. Rep., 1900-1901, Part 3, pp. 579-627, \Washington, 1902.) GRABAU, A. W. Studies of Gastropoda. (Am. Nat., vol. 36, Dec. 1302, pp., 917-945.) GILMORE, C. W. Discovery of teeth in Baptanodon, an ichthyosaurian from the Jurasic of Wyoming. (Science, vol. 16, Dec. 5, 1902.) HAY, O. P. Description of a new species of Cladodus (C. formosus) from the Devonian of Colorado. (Am. Geol., vol. 30. pp. 373-374, Dec. 1902.) HAYDEN, H. E. Anthracite coal in Wyoming valley. (Proc. Wyo. Hist. and Geol. Soc., vol. 7, 1901, p. 29. Wilkesbarre, 1902.) HOBBS, W. H. Instanee of the action of the ice-sheet unon slender projecting rock masses. (Am. Jour. Sci., vol. 14, Dec. 1902, pp. 399-404.) Authors Catalogue. 61 HOVEY. E. O The eruptions of La Soufriére, St Vincent, in May, 1902. (Nat. Geog. Mag., vol. 13, pp. 444-459, Dec., 1902.) JAGGAR, T. A., JR. The next eruption of Pelée. (Science. vol. 16, p. 871, Nov. 28, 1902.) JOHNSON, D. W. . On some Jurassic fossils from Durango, Mexico. (Am. Geol., vol. 30, pp. 370-372, Dec., 1902.) KOENIG, G. A. New species of melanochalcite and keweenawite, with notes on some other known species. (Am. Jour. Sci., vol. 14, Dec., 1902, pp. 404-416.) LUQUEUR, L. Mcl. (ALF. J. MOSES AND). Notes on recent mineralogical literature. (Reprinted from the Journal of Applied Microscopy, vols. 3 and 4, and from the School of Mines Quarterly, vol xxii.) McGEE, W. J. ¢ Geest. (Am. Geol., vol. 30, pp. 381-384, Dec., 1902.) MERRILL, F. J. H. Twentieth report of the State Geologist. (N. Y. State Museum, 54th annual report, p. 189, Albany, 1902.) MOSES, ALFRED J. (AND L. Mcl. LUQUEUR.) Notes on recent mineralogical literature. (Reprinted from the Journal of Applied Microscopy, vols 3 and 4, and from the School of Mines Quarterly, vol. xxii.) RUSSELE, tic GCG. Volcanic eruptions on Martiniaue and St. Vincent. (Nat. Geog. Mag., vol. 13, pp. 415-436, Dec., 1902.) WILLIS, BAILEY. Stratigraphy and structure. Lewis and Livingston ranges, Mon- tana. (Bull. G.S.A., vol. 13, pp. 305-352, pls. 46-538, Nov., 1902.) WILLISTON, S. W. Restoration of Dolichorhynchops osborni, a new Cretaceous plesiosaur. (Kans. Univ. Sci. Bull., vol. 1, Sept., 1902, pp. 241-244.) WILLISTON, S. W. Notes on some new or little known extinct reptiles. (Kans. Univ. Sci. Bull., vol. 1, pp. 247-254, Sept., 1902.) WILLISTON, S. W. On certain homoplastic characters in aquatic air-breathing ver- tebrates. (Kans. Univ. Sci. Bull., vol. 1, pp. 259-266, Sept., 1902.) WILLISTON, S. W. The Laramie-Cretaceous of Wyoming. (Science, vol. 16, p. 952, Dec. 12, 1902.) WILLIAMS, E. H. Kansas glaciation and its effects on the river system of northern Pennsylvania. (Proc. Wyo. Hist. and Geol. Soc., vol. 7, 1901, pp. 21- 28, Wilkesbarre, 1902.) 62 The American Geologist. | ease CORRESPONDENCE. APATITE CRYSTALS, ANTWERP, New York. The following is the analysis of some crystals of apatite that were obtained near Antwerp, Jefferson Co., New York, some time ago. They were olive green prisms and were about two centimetres long, and eight millimetres in di- ameter, The analysis was made in the chemical laboratory of Cornell college by assistant Frank L. Hann. CaO 48.20 P20; 41.00% Cas(PO,): 89.20% SiO: 0.60 Al.O; 9.00 CaF 1.20 100.00% Mount Vernon, Iowa, Dec. 24, 1902. NICHOLAS KNIGHT. Fatt ExcursIoNs OF THE GEOLOGICAL DEPARTMENT, CoLUMBIA UNTI- versity, The weekly fall excursions of the Columbia geological de- partment closed, as usual, on the last Saturday in November. These are usually half-day excursions and take place on Saturday forenoon. Local sheets of the U. S. Geological Survey, note books, hammers and compasses are necessary for each participant. Each excursion is guid- ed by at least one officer of the department. New York city, especially Harlem and its environs, is an ideal place for short excursions of ex: ceptional geological interest. The university itself is situated upon the area of the Manhattan schist which is believed by state geologist Mer- rill to be metamorphosed Hudson River shale. This schist is exceed- ingly full of pegmatyte dikes in which there is frequently a great abundance of tourmaline. There are also veins or interbedded strata which are now hornblende. These are of problematic origin. In places they are very numerous varying in width from a fraction of an inch ta several feet and in length extending at times through an entire outcrop. several hundred feet. They frequently end very abruptly. The Man- hattan schist is at times so full of garnets as to merit the name of gar- net schist. This is well shown just north of the convent of the Sacred Heart on 135th St. near Amsterdam Ave. There are fine examples of pinched folds in the Manhattan schist where folded in the more gneis- soid strata. The schist is frequently pinched into complete cylinders. These were noted and described many years ago by Prof. Dana. The Manhattan schist rests, apparently conformably, upon the In- wood limestone. This is a very coarsely crystalline rock which weath- ers into a coarse lime-sand. On account of its great solubility it usu- ally occupies the valleys. Prof. Hobbes has lately readvanced an old theory, held. by Dana and others, of the fault formation of these val- leys. The valley breaking through Morningside Park ridge at 125th Correspondence. 63 St. and forming the valley between the hights of Columbia University and those upon which the convent of the Sacred Heart is situated is frequently brought forward in support of this view. In this rock at the contact with pegmatyte dikes very good specimens of foetid quartz, phlogopite, white pyroxene and brown tourmaline are obtained. The Inwood limestone, called by Merrill Cambro-Silurian, is exposed at 7th Ave. and 155th St-, and at the typical locality Inwood, immedi- ately north of Fort George (Amsterdam Ave. and rioth St.) Berieath this limestone is the Fordham gneiss which is thought te be of igneous origin and of Archean age. An unquestioned exposure of this rock is not known upon Manhattan island; but north of the island are abundant exposures. Above the Manhattan schist is the Triassic sandstone which is well shown on the western side of the Hudson. The base of this sandstone a conglomerate, is well exposed in a cut made by the West Shore R. R. at Stony Point. The sandstone is penetrated by the Palisade sheet of diabase. The sandstone both above and below the diabase is baked into a hornfels in which the characteristic metamorphic minerals are usually present. In places this becomes a tourmaline hornfels from the great development of that mineral. The effect of the cool walls upon the intruded igneous mass is very evident as one follows the sheet from its lower to its upper contact on the sandstone. The middle of the sheet is very coarsely crystalline but becomes quite fine grained as the wall is approached. Mr. A. L. T. Quereau has lacely given the re- sults of his study on the subject in the School of Mines Quarterly, Vol. XXIII. This diabase sheet with its columnar jointing forms the well known Palisade on the west bank of the Hudson river. The lower contact is well shown at the 130th St. ferry. Here is an excel- lent place to note the gradual change in the texture of the diabase as the Palisades are ascended. The upper contact is shown at the tunnel of the West Shore R. R. at 34th St. ferry. Besides the intruded sheet there are above n, farther west in New Jersey three surface flows; for the upper surface of each is amygdaloidal. The first or lowest flow is well shown at Feltyville. At the Great Notch on the Green- wood Lake division of the Erie R. R. is an excellent place for the collection of minerals. These occur between two of these surface flows in the interstratified baked shale. Here are found quartz, cal- cite, analcite, heulandite, stilbite, prehnite, natrolite, datolite, pectol- ite, chabazite and other minerals. Fatlts are quite numerous in the Triassic, one of which is exposed at Kingspoint near Hoboken. Another interesting rock which the classes always visit is serpen- tine. It is well exposed in Hoboken at Castle Point. The problem of its origin is still debated, but is thought by most to be an altered peridotyte or pyroxenyte, since the presence of pyroxene, amphibole and olivine has been determined. The processes of serpentinization are however nearly complete. This is the home of various magnesian minerals as brucite, nemolite and magnesite. Chromite is also abundant. 64 The American Geologist. Janene: Good illustrations of peneplains are seen here on all sides in the uniform hights to which the different rocks have been eroded. The gneiss schists sandstone and dikes rocks varying much in hardness, have been eroded approximately to the same level. Many other points in the physiography of the region are impressed upon the students in their trips. Glacial drift and striations are abundant in and about the city. On election day an all-day trip is taken to some point within fifty miles of the city. This fall it was up into the Hudson River high- ’ lands. The West Shore R. R. was taken to Grassy Point and from there the class walked to Ft. Montgomery. On the way excellent ex- posures of Champlain clays were noticed and the consequent develop- ment of the brick industry. Near Stony Point where lunch was eaten, the Basal Triassic conglomerate and the contact of mica schist on the Cortlandt eruptive series were noticed. North of Stony Point fine exposures of Cambrian limestone were examined carefully for fossils but none were found: Farther north still the. class entered the high- lands with its Archean gneiss, trap dikes and celebrated scenery. HENRY W. SHIMER. PERSONAL AND SCIENTIFIC NEWS. s IN THE WINTER COURSE OF LECTURES of the Chicago Acad- emy of Sciences are the following geological topics: The Yel- lowstone National Park, Charles Truax; Some methods of Geological field work, U: S. Grant; Flying reptiles, S. W-: Williston. Tue Unrrep STATES GEOLOGICAL SuRVEY has commenced another series of publications, denominated “Professional Pa- pers.” The first of this series.is that of Dr. A: H. Brooks, re- cently issued, ‘Preliminary report on the Ketchikan Mining District of Alaska, with an introductory sketch of the geology of southeastern Alaska.” GEOLOGICAL SOCIETY OF WASHINGTON. At the meeting of the society on January 14th the following program was pre- sented: ‘“‘An instance of replacement of mortar by metallic copper,’ Arthur C. Spencer; “A genetic classification of ore deposits,” Walter H. Weed. The discussion of the last paper was led by Messrs. Emmons, Lindgren, Spurr and Ransome. Tue Baro Furnace Merteorire fell at Bath Furnace, Kentucky, on the night of November 15. It was found buried about a foot and a half in the ground. Its weight is about five pounds. It was observed from New Orleans northward. It is now in the Ward-Coonley collection, on deposit in the American Museum of Natural History. It is of gray stony Personal and Scientific News. 65 . material, and. is supposed to be only a part of the original mass that entered the earth’s atmosphere. Dr. J..W. SPENCER, accompanied by Mrs. Spencer, left on Jan. 7 for the Windward islands, intending to be absent for over three months, where six years ago he also spent over five months. Dr. Spencer is investigating the submarine Carib- bean ridge extending. to South America. He has found that an Oligocene white limestone underlies the St. Martin group and Antigua, and he will re-examine these islands with the view of more detail, the volcanic phenomena being a second- ary consideration. THE AMERICAN INSTITUTE OF MINING ENGINEERS will hold its eighty-third meeting (the thirty-third annual meeting) in Albany, New York, beginning February 17, 1903. The headquarters and places of session have not yet been an- nounced. It is expected that at this meeting trips will be tak- en to the shops of tihe General Electric Company, and there is a promise of several interesting papers on electricity as ap- plied to mining. The Institute has accepted an invitation to hold its August meeting in British Columbia, and in connec- tion with this meeting there will be an excursion to Alaska. The library of the Institute now numbers some ten thousand volumes on mining and geology, and this library is now acces- sible for the use of members. New Mexico ACADEMy oF SciENcEs. At the winter meet- ing of the New Mexico Academy of Sciences, held at I.as Vegas in the assembly hall of the Normal University, Decem- ber 22-23, Hon Frank Springer was elected president, Dr. Charles R. Keyes, vice-president, and Prof. W. G. Tight, sec- retary-treasurer. The following geological papers were read: Theory of Meteoric Agglomeration and the Migration of Ore Materials, by Dr. Charles R. Keyes; History of the Rio Grande at Albu- querque, Prof. W. G. Tight ; Louis Agassiz, by Mr. Frank Springer; Analyses of New Mexico W: aters, by Prof. F. C. Lincoln; Relations of Moisture in Mesa Soils, by Prof. C. L. Magnusson; Gypsum Deposits of New Mexico, by Mr. Harry Herrick; Geological Structure of New Mexican Bolson Plains, by Dr. Charles R. Keyes; Sources of Errors in Our Land Sur- veys, by Prof. O. R. Smith; Geological Sketch of the Sandia Mountains, Dyeleror. NW. -G:. Tight. A committee of three, consisting of Dr. Charles R. Keyes, Hon. Frank Springer and professor W. G. Tight, was ap- pointed to present the matter of a geological survey to the New Mexican legislature this winter. Resolutions were passed recommending to Congress the desirability of establishing a National Ethnological Park north of Santa Fe, in one of the richest districts of prehistori¢ ruins 66 The American Geologist. Jana eoee in the world. The object is to preserve this intensely interest- ing region from further depredations and vandalism. THE LATE MEETINGS OF THE GEOLOGICAL SOCIETY OF AMERICA, of the American Association for the Advancement of Science, and of over twenty other scientific societies, at Washington, were an eventof noordinary importance for Amer- ican science. No such gathering of scientific men resident in America ever before took place. The only meetings that could be compared with it were those of the joint meetings of the 3ritish and American Associations for the Advencement of Science, or some of the international congresses held in Amer- ica. The number in attendance on the Geological Society of America was about 115, the largest meeting hitherto having been 80. Section E of the Association and the Geological So- ciety held joint meetings, the papers listed being more than 90. Most of these were presented in the meeting room of the U.S. Geological Survey, but a series of papers relating to the West Indies were given in the Columbian University. An illustrated popular lecture on the volcanic phenomena of Mont Pelée was given by Prof. I. C. Russell, and the retiring ad- dress of president Winchell was given in the New Willard hotel. Mr. John Hays Hammond gave a popular lecture at the Lafayette Opera ‘House, on “King Solomon’s mines, or the mines of Ophir.’ The week was diversified with numer- ous dinners, luncheons and receptions and with visits to var- ious public buildings. Owing to the crowded condition of the meetings, several of the sections and affiliated societies suffered from the friction and the duplication of the machinery of administration, but it was only for the relief of Section E that the Council of the Association took general action, in the adoption of the follow- ing resolution : See solved, That Section E is hereby authorized to suspend its sci- entific program of the reading of papers at any winter meeting when the Geological Society of America meets in conjunction with the As- sociation; provided, that the Geological Society includes in its pro- gram the papers of worthy character offered by members of the Sec- tion who are not fellows of the Society. The Association, however, requires each Section to hold at least one afternoon meeting, during each general meeting of the Association when a program of general interest shall be presented. At such meeting it is likely that in future the ad- dress of the retiring chairman of Section E will be heard. The new president of the Geological Society is S. F. Em- mons, Washington, and the vice- president, Section EF, is IT. C. Russell, Ann Arbor. The next annual meeting will be convo- cation week 1903-04, at St. Louis. The new president of the American Association is Carroll D. Wright, Washington. Saw 9 qiiseiwy et} oyster) serawyay) (wn5d AD) mssvant “ft ez cre.) WLIHI0D a Ly) Fit tee = aN > a2 XS Z, SOV SLL NEFF SES VAIS YIN OES xX 9 \ Ar Rf RRR ae, OA APCR RE SRD OIIGFS oO NS MAA SSN Ye OLS PSO SXRD As x ALLO GTYS SY SOREN IR X'S x “yi ee RRR NS ON Cy KWROKR rete onatataes wLRSSS S SSRN RRR eS \ SSN ESS S th POR SSP wr NS SN ~ aS NS A N POIANA AY SRN NAO GD NVOVSHH LaazeT¥ 5 bag SAA RAS AN > a NAN \N ¥ SAN SSS SSNS A ‘ SSANNS NANA SS ‘wold SON IMas YNHd INS wil andwanonay «e3awal and 40 Apo10a") wweww ‘Tan tLernoanoOen NVOIBARY BO OVAL Id ZAWAL / WLLL iJ li Mae ci ny — Vid XD h 2 7/ ysl 7 SSG SS uM LaVentane mm Tue AMERICAN GEOLOGIST, VOL. XXXI. PLATE V. Ax y = a Sf AIA Nia oNe o Sa lt Ruer - ne AAS No Ne 0 = t \ SEX e AV AATAlAlAlalal ate ONO \ REPRESSES : Alala alte ore NS CSRS re a, Plersiecene SPV AIAIA\Alalalala\r DOS eco Shales bps tocene c ocené Alala|salaialalalalala OAS © Ce eemHeues hood ft. vert @- Cretacéeus AJANIATAIALAIAIAIA la lA S 4.- Jurassic i J:- Tred Beds AM ALATATAIALAIALALA IA IA I Granite Sea Level Jemer mts, mre ctet® Veen i : eqeten lei ftecene §-- Granite wert t+4F9 0 Tlioce he 0 - Focene B- Basalt “Cretacecus -Red Beds - Jurassic - Fer His - Puerco = Chr bent serous i Fe 5000 fi. verf bOMieS @ Pleistocene. J: kh. Granite . Pliocene. ‘ Sood ft. vert. Eocene ©. Cretaceous. 5 miles, J Jurassic Sea __Level. Red Beds. eee eee SS ee Coe —_—_———— SSS SSS ———— ——————————————————— PLATE V. THE rn tOAN GEOLOGIST. Vor. XXXI. FEBRUARY, 1903. Not 2. GEOLOGY OF THE JEMEZ—ALBUQUERQUE REGION, NEW MEXICO. By ALBERT B. REAGAN. PLATES IV-XII. CONTENTS. Page. Rear ACE SCI MDELOM rivet cle siasehqos. Y.,-Pal., 11, 1852, \‘p. 327, plogasiies: 8a-8d (specitners in Amer. Mus. Nat. Hist., No. /,). Spirifer eriensis Grabau, Bull. Geol. Soc. Amer., XI, 1900, p. 366, pl. 21 igs a2a2p: This shell from Herkimer county and Schoharie is very closely related to S. modestus of Maryland (this species is restricted to the Manlius), and it is a question whether the two forms are distinct. S. modestus may have a few more plica- tions, but these as a rule are nearly obsolete, though fully twenty-five per cent of the specimens have them as strongly developed as in S. eriensis. It is found also in the “Water- lime” (Rondout) at Schoharie. Spirifer modestus corallinensis (Grabau'. Spirifer crispus Hall (non Hisinger), Nat. Hist. N. Y., Pal., II, 1852, p. 328, pl. 74, figs. ga-gh. Spirifer crispus var. corralinensis Grabau, Bull. Geol. Soc. Amer., XI, 1900, p. 352 (the varietal name is improperly constructed). This is not the Rochester shale S. crispus which has well developed plications and from which S. vanuxemi apparently descended. This Cobleskill species is almost devoid of plica- tions and is closely related to S. modestus of the Maryland Manlius. The latter is always a larger shell and as a rule is more subquadrate, with a tendency to have distinct plications. It is also a common shell about Litchfield, Herkimer county, New York. Whitfieldella (?) nucleolata (Hall), Atrypa nucleolata Hall, Nat. Hist. N. Y., Pal., II, 1852, p. 328,. pl. 74, figs. T0a-Tom. d Wiutheldella cf. rotundata Grabau, Bull. Geol. Soc. Amer., XI, 1900, 368, pl. 22, figs. 3a, 3b. Manlius Formation of New York.—Schuchert. 167 In Herkimer county this species is associated with WV. (?) sulcata. Whitfieldella (?) sulcata (Vanuxem). Atrypa sulcata Vanuxem, Geol. N. Y., Rep. Third Dist., 1842, p. 112, fig. 5.— Hall, Ibidem, Fourth Dist., 1843, p. 142, fig. 5. Merista bisulcata Hall, Nat. Hist. N. Y., Pal., III, 1859, p. 253 (error for Vanuxem’s 4. sulcata) Whitfeldella sulcata Grabau, Bull. Geol. Soc. Amer., XI, 1900, >. 367, pl. 22, figs. 2a-2d. This is a characteristic shell of the Cobleskill. It occurs commonly about Litchfield, New York. Rhynchonella (?) lamellata (Hall). Atrypa lamellata Hall, Nat. Hist. N. Y., Pal., II, 1852, p. 320, pl. 74, figs. I1a-rrh. Also found in the “Waterlime” (Rondout) at Schoharie and in the Cobleskill about Litchfield, N. Y. This shell has an extended distribution in New Jersey, Pennsylvania, Mary- land, and West Virginia. In New York it does not appear to pass far above the Cobleskill but in Maryland it ranges through 400 feet of the upper Salina and through 50 feet or more of the lower Manlius. 3 Rhynchonella (?) litchfieldensis n. sp. Airypa sp., Hall, Nat. Hist. N. Y., Pal., Il, 1852, p. 330, pl. 74, figs. 111 and 12. This species is one of a group represented in the Rochester shales by R. (?) neglecta and in the Helderbergian by R. (?) transversa. It differs from the former in having more plica- tions with the fold and sinus narrower and! less pronounced. It is more closely related to R. (?) transversa, but never at- tains the size of this species, nor is the fold and sinus so broad. The figured specimen is from Wheelock’s farm, Litchfield township, Herkimer county, New York, and is in the U. S. National Museum. (No. 34634.) 168 The American Geologist. _ March, 1903. Tellinomya? equilatera Hall, Nat. Hist. N. Y., Pal., II, 1852, p. 330, pl. 75, figs. ta-1d. : This may be a Cycloconcha or Ctenodonta. vicula subrecta Wall, Nat} Hist, °N. Y., Pal., Il, 1852,,- The American Geologist. March, 1903, lake Beulah, Elkhart lake, Oconomowoc and other lakes. of Waukesha county, the Chain-o’-Lakes in Waupaca county, Delavan and Lauder- dale lakes, Green lake, Big Cedar lake, and lakes Mendota and Mon- ona, adjoining Madison. Much attention is given to the effects of glaciation in producing the multitudes of small lakes in this region, and to the, action of the lakes in modification of their shores, Lake Winnebago, larger than any of these, but comparatively shal- low, is expected to be the theme of another bulletin; and an atlas of the chief lakes of the state is in preparation. Lake Mendota, having an area of 15 square miles, is the largest here described; and Green lake, measuring 237 feet in depth, is the deepest. The maps show admirably the contour of the lake beds, which, not less than their shores and the surrounding country, give evidences of the glacial history to which mainly they owe their origin. W. U. The Origin of Certain Place Names in the Umted States. By HEnry GANNETT. Bulletin of the U. S. Geol. Survey, No. 197. Pages 280; Washington, 1902. . Historians and antiquaries will welcome this very satisfactory com- pilation of the origin and meaning of about seven thousand geographic names, representing, though far from completely, all parts of our country. This work may desirably be much further extended, for which the author invites ‘criticisms and additions, with a view to ob- taining in the future all possible information on this subject.” It is a field of especial attractiveness for students of geography, history, and philology. Very advantageously may our state historical societies gather all details in their respective states, as is now being done in Minnesota, for their own publications and for contribution to the great work planned, and thus begun, by our national survey . W. U: Bornholms Paradoxideslag og deres Fauna, af Karu A. GRONWELL [ Danmark’s geologiski Undersogelse, 11 Rekke Nr. 13, Kjobenhavyn, 1902. | This admirable and comprehensive essay gives an excellent review of the epitomized sections of the Cambrian terrane of the island of Bornholm in the Baltic sea. Previous to the issue of this publication, work had been done on the Cambrian of this island by Prof. F. Johnstrup and others, and the fauna obtained compared with those of localities in Sweden and Norway, but this work goes much more thoroughly into the treat- ment of the fauna in all its aspects than has hitherto been attempted. The collections are chiefly from two localities—Lcesaa and Bor- regaard at Aa. When it is understood that the whole thickness of the Paradoxides at one of these localities is but little over 2 metres, and at the other not much over 3, it will be seen of how little bulk the Middle Cambrian is in southern Scandinavia. Mr. Gronwell was unable to find the full development of the Paradoxides beds, as seen at Andrarum in Sweden, on this island, Review of Recent Geological Literature. - 187 and gives a more condensed view of the succession, condensing the six lower zones of Andrarum into one, that of Paradoxides tessini, but he divides this into three sub-zones, beginning with that of Con- ocoryphe exsulens. An interesting feature of these Bornholm sections is that while at one locality where the limestone of C. exsulens is present, at the other there is a bed of clay. Hence Mr. Greenwell assumes that this is a residual clay due to the decomposition of the limestone, and removal by solution of the lime. The fossils in the gray clay at Lesaa show it to be of the same age as the limestone of Aa. At the base of the Exsulens limestone there was at Bornholm an erosion, cutting out about 5 metres of measures, as known on the Swedish peninsula. The genus Agnostus is well represented in the Paradoxides beds of Bornholm, both as regards individuals and the number of species, Mr. Greenwell describes twelve new species, or varieties of species, already known. Microdiscus is found in two forms, scanicus and eucenirus, the au- thor reduces the latter to a form or mutation of the former. Conocoryphe is quite fully treated and shown to contain four sub- genera: (1) Conocoryphe, Corda (s. str.), (2) Erinnys, Salter, (3) Ctenocephalus, Corda, and a new subgenus (4) Liocephalus, estab- lished to contain C. impressa Lnrs., C. lyelli Salt, and probably Hol- ocephalina, Salt. [It seems doubtful if the last genus should go in its entirety to Conocoryphe, especially H. inflata]. Three new species are described under this section. Paradoxides. Mr. Crénwell is inclined to think, P. brachyrrachis Lnrs, a separate species from the. Bohemian P. rugulosus, to which it has been referred. He finds a variety of P. sjogreni Lnrs, (nepos) of much later time than the typical form. Dorypyge, Dames, is represented in two new species of the Born- holm beds, which helps to give this genus a lower position than orig- inally determined by Dames, as one was found in the Exsulens lime- stone, and both below the Andrarum limestone. This is parallel to the conditions in eastern North America, where the genus is found in beds with or below the representative of Paradoxides tessini, [The occurrence of these early forms of the genus seems related to shallow water and rough shores.] Corynexochus has been found in good examples, including a new species, C. bornhomensis. Anomocare is represented by forms already described (by Angelin) and by a new one, A. angelini. Of Liostracus, two new species are described, and of Ptychoparia, one. Solenopleura has one new species, and Agraulos, one. [It seems questionable whether this form should be referred to Agraulos; it might with equal propriety go to Anomocare.| A solitary ostracod and gasteropod give further rarity to the fauna. Comparisons are made with Paradoxides beds in other parts of the world, as various parts of Scandinavia, Wales, Bohemia, North Amer- ica, China, &c. A very nice distinction, only possible in such a region 188.7) 4 The American Geologist. Mir Cie oue as Scandinavia, where the Cambrian fossils have been so thoroughly worked out, is that between the district of S.W. and N.E. Scandinavia, where not only were the physical changes to some extent, distinct. but occurrence or absence of the subfaunas was consequent upon these differences. Four superb plates of figures, chiefly of the new species and forms, add to the interest and usefulness of the volume. With this book in hand of those of Linnarsson, Brogger, Wallerius and others, one is able to get a very satisfactory understanding of the Cambrian species of the Scandinavian peninsula and islands; including many species of Angelin, upon which much obscurity rested owing to imperfect figures and very brief diagnoses of the species in the ‘“‘Paleontoligica Scandinavica.” An English summary of the contents is bound up with this book. G. F. iM: MONTHLY AUTHOR’S CATALOGUE OF AMERICAN GEOLOGICAL LITERATURE ARRANGED ALPHABETICALLY, ADAMS, G. I. Physiography and general geology of the lead and zine region of the Ozark region. (22 Ann. Rep., U.S.G.S., part 2, pp. 69-94, 1901.) ADAMS, GEO. I. Geology and water resources of the Patrick and Goshen Hole quadrangies, in-eastern Wyoming and western Nebraska. Wat. Sup. ie Papiy WSN Gs wINO wi. sODs OO, OLS del o Oz ASHEEVAtGraric The eastern interior coal field. (22 Ann. Rep., U.S.G.S., 1901, part 8, pp. 333-367, pls. 22-24.) BAIN, H. F. Preliminary report on the lead and zine deposits of the Ozark region. (U. S. Geol. Surv., 22 Ann. Rep., 1901, part 2, pp. 23-227, pls. 6-25.) BAIN, H. F. The western interior coal field. (22 Ann. Rep., U.S.G.S., 1901, part 3, pp. 333-367, pls. 22-24.) BARRELL, JOS. H. Microscopical petrography of the Elkhorn mining district, Jeffer- son county, Montana. ((22 Ann. Rep., U. S. G. S., 1901, Part 2. pp. 511-549, pl. 62.) BROADHEAD, G. C. Biographical sketch of Dr. A. Litton. (Trans. St. Louis Acad. Sci., 1902. pp. xxiv-xxvi, portrait.) Author's Catalogue. 189 BROOKS, A. H. The coal resources of Alaska. (22 Ann. Rep., U.S.G.S., 1901, part 3, pp. 515-573, pl. 35.) CAMPBELL, M. R. Reconnaissance of the borax deposits of Death valley and Mo- have desert. Bull. 200, U.S.G.S., pp. 22, plate 1, 1902.) CAMPBELL, M. R. (D. White and) The bituminous coal field of Pennsylvania. (22 Ann. Rep., U.S. G.S., 1901, part 3, pp. 128-214.) CUMINGS, E. R.’° - Morphogenesis of Platystrophia; a study of the evolution of a paleozoic brachiopad. (Am. Jour. Sci., vol. 15, Feb. 19038, pp. 121-1387.) DAY, DAVID F. Mineral resources of the United States. calendar year 1900. U.S. G.S., (with contributions by Messrs. Birkinbine, Swank, Kirchhoff, Pratt, Brooks, Oliphant, Parker, Kunz, Kiibel and Peale.) pp. 927, Washington, 1901. DAY, DAVID F. Mineral Resources of the United States, Calendar year, 1901. U.S. G. S., 1902, pp. 996. Cwith contributions by Birkinbine, Swank, Roberts, Kirchhoff, Struthers, Pratt, Snelling, Parker, Oliphant, Kunz, Parsons, Vaughan, Ries, and Hovey.) DARTON, N. H. Catalog of photographs belonging to the Geological Society of America. (Bull. G.S.A., vol. 13, pp. 377-474, Dec. 1902.) DICKSON, C. W. Condition of platinum in the nickel-copper ores from Sudbury. (Am. Jour. Sci., vol. 15, Feb., 1903, pp. 137-140.) DILLER, J. S. Topographic development of the Klamath mountains. Buli. 196, U.S.G.S., pp. 69, pls. 13, 1902. DRYER, C. R. The use of the word geest in geology. (Science, vol. 17, Feb. 6, 19038, p. 234.) ELLS, R. W. The progress of geological investigation in Nova Scotia. (Trans. N. Sco. Inst. Sci., vol. 10, 1901-1902, pp. 483-446.) ELDRIDGE, GEO. H. The asphalt and bituminous rock deposits of the United States. (22 Ann. Rep., U.S.G.S., Part 1, pp. 219-452, pls. 25-58, 1901.) BUREER Men: The Gaines oil field of northern Pennsylvania. (22 Ann. Rep., U.S.G.S., part 2, 1901, pp. 573-629, pls. 35-43.) GANNETT, HENRY. The origin of certain place names in the United States. Bull. TOT MWe Gass Dpr 280. 1902. GANNETT, HENRY. A. Gazetteer of Cuba. Bull. 192, U.:S. G. S., pp. 118, pls. 8, 1902. 190 The American Geologist. saaen es GANNETT, HENRY. A Gazetteer of Texas. Bull. 190, U. S. G. S., pp 162, pls. 8, 1902. GREENE, GEO. K. Contribution to Indiana paleontology, part IX, pp. 98-109, pls. 3. New Albany, 1903. GRISWOLD, W. T. The Berea grit oil-sand in the Cadiz quadrangle. Bull. 198, U.S. GS; pp: 438;- ply 2, 29.02: HASELTINE, R. L. The bituminous coal field of Maryland. (22 Ann. Rep., U.S.G.S., 1901, part 3, pp. 215-226.) HAY, O. P. Bibliography and catalogue of the fossil vertebrata of North America. Bull. 179, U. S. G. S., pp. 868, 1300. HAYES, C. W. The coal fields of the United States. ((22 Ann. Rep., U. S. G. S., part 3, 1901, pp. 7-24, pl. 1.) HAYES, C. W. The southern Appalachian coal field. (22 Ann. Rep., U. S. G. S., 1901, part 3, pp. 227-265, pls. 138-15. HOBBS, W. H. The old tungsten mine at Trumbull, Conn. (U.S. Geol. Surv., 22 Ann. Rep., 1901, Part 2, pp. 7-22, pls. 1-5.) HOLMES, W. H. Fossil human remains found near Lansing, Kansas. (Am. Anth., n.s., vol. 4, Oct.-Dec., 1902, pp. 7438-752, pls. 31, 32.) KEMP, J. F. Geological relations and distribution of platinum and associated metals. Bull. 193, U.S.G.S., pp. 95, pls. 6, 1902. KNOWLTON, F. H. Fossil flora of the John Day basin. Bull. 204, U.S.G.S., pp. 113, DUS tel OO. LANE, A. C. The northern interior coal field. (22 Ann. Rep., U. S. G. S., 1901,. part 3, pp. 307-883, pls. 20-21.) LINDGREN, WALDEMAR. The gold belt of the Blue mountains of Oregon. (22 Ann. Rep., U.S. G.S.,-1901,. Part 2, pp. 561-776, pls. 63-78.) LINDGREN, WALDEMAR. Tests for gold and silver in shales from Western Kansas. Bull. 202s. GIS. DDvL9 19028 MURDOCH, L. H. Why Great Salt Lake has fallen. (Am. Geog. Mag., vol. 14, Feb. 1903, pp. 75-77.) : NEWERE Ect: Report of progress of stream measurements for the calendar year 19015 (Wat. Sup. Ir. Pap; WUiS..G.S:, §No. 75,40. 246,. pl. sat 903. Author's Catalogue. IOI ORTMAN, A. E. The geographical distribution of fresh-water decapods and its bearing upon ancient geography. (Proc. Am. Ph. Soc., Vol. 41, April- Dec., 1902, pp. 267-399.) PETERSON, C. A. The Clayton stone ax. (Rec. Past., vol. 2, Jan., 1963, p. 26.) PRATT, J.H. The mining industry in North Carolina during 1901. WN. C. Geol. Surv., Economic paper, No. 6, pp. 102, 1302. RANSOME, F. L. A report on the economic geology of the Silverton quadrangle, Colorado. Bull. 182, U. S. G. S., pp.1258, pls. 15, 1901. RANSOME, F. L. The ore deposits of the Rico mountains, Colorado. ((22 Ann. Rep., Uses. G.S., Part 2, pp. 231-397, pls. 26-39, 1901.) REAGAN, A. B. Geclogy of the Jemez--Albuquerque region, New Mexico. (Am. Geol., vol. 31, pp. 67-111, Feb., 19038, pls. 4-10.) RUSSEEE. EUG: Geology and water resources of the Snake river plains of Idaho. Bull 199, WU-S.G.S., pp. 192. pls. 25, 1902. RUSSELL, |. C. Timber lines. (Am. Geol., vol. 31, Feb., 1903. p. 121.) RUSSELL, IC: The Portland cement industry in Michigan. (22 Ann. Rep., U.S. G.S., 1901, part 3, pp. 629-687, pls. 44-46.) SCHUCHERT, CHAS. ; On the lower Devonie and Ontaric formations of Maryland. (Proc. U.S. Nat. Mus., vol., 26, pp. 413-424, 1903.) SCHUCHERT, CHAS. Morse on living brachiopods. (Am. Geol., vol._31, pp. 112-121, Feb., 1903.) SINCLAIR, W. J. Mylagar.odon, a new rodent from the upper Jehn Day, of Oregon. (Am. Jour. Sci., Vol. 15, Feb., 1903, pp. 148-145.) SMITH, G. O. The Pacific coast coal fields. (22 Ann. Rep., U.S. G.S., 1901, part 3, pp. 473-515, pls. 31-34.) STOEK, H..H. The Pennsylvania anthracite coal fields. (22 Ann. Rep., U.S.G.S., 1901, part 3, pp- 55-119, pls. 6-10.) STORRS, L. S. The Rocky mountain coal field. (22 Ann. Rep., U.S.G.S., 1901], part 3, pp. 415-473, pls. 29-30.) TAFF, J. A. Chalk of southwestern Arkansas, with notes on its adaptability to the manufacture of hydraulic cements. 22 Ann. Rep., U.S.G.S., 1901, part 3, pp. 687-742, pls. 47-53.) 192 The American Geologist. Merch, ta TAFF, J Aw The southwestern coal field. (22 Ann, Rep., 1901, part 8, U.S. G.S., po. 367-415, pls. 26-28.) VAN HISE, C. R. Introduction to Bain’s Report on the lead and zine deposits of the Ozark region. (23 Ann, Rep. U. S. G. S., part 2, pp. 33-60, 1901.) WALCOTT, C. D. Report of the director, CU.S.G.S.), 22 Ann. Rep., 1900-'01, in four parts, Washington, 1901, WATSON, T. L. Copper bearing rocks of Virgilina copper district, Virginia and North Carolina. (Bull. GS. A., vol. 18, pp. 368-376, pls. 54-56, Nov,, 1902.) WEED, W. H. Geology and ore deposits of the Elkhorn mining district, Jefferson county, Montana. (22 Ann. Rep., U. S. G S., 1901, Part’2, pp. 899- 510, pls, 42-62.) WEED, W. H. ' Notes on a section across the Sierra Madre occidental of Chihua- hua and Sinaloa, Mexico. (Am. Inst. Min. Eng., Mex. Meet., Nov. 1901, 1902.) WEEKS, F. B. North American formation names, bibliography, synonymy and distribution. Bull. 191, U. S. G@ S., pp. 488, 1902. WEEKS, F. B. Bibliography and index of North American geology, paleontol- ogy, petrology, and mineralogy for the year 1901. Bull. 208, U. S. G. S., pp. 144, 1902. WEEKS, F. B. Bibliography of North American geology, paleontology, petrol- ogy, and mineralogy, for the years 1892-1900 inclusive. Bull. 188, U.S. G.S., pp. 717, 1902. WHITE, D. (AND M. R. CAMPBELL) The bituminous coal field of Pennsylvania. (22 Ann. Rep., U.S G.S., 1901, part 3, pp. 128-214.) WOODWORTH, J. B. The Atlantic coast Triassic coal field. (22 Ann. Rep., U.S. G.S., part 8, 1901, pp. 26-55, pls. 2-5.) PERSONAL AND SCIENTIFIC NEWS. Proressor D. E. Wriiiarp of the Normal school at May- ville, N. Dak., has been appointed professor of geology at the state agricultural college at Fargo, successor to C. M. Hall, lately deceased, Personal and Scientific News. 193 _ Dr. G; P. Merrite or rue U. S. Narionat Museum has been appointed expert special agent of the Census office in con- nection with the collection of statistics relating to stone quar- ries, The appointment in no way affects Dr. Merrill’s posi- tion as head curator of geology in the museum. Mr. H. W. Suimer has been appointed lecturer in Histor- ical Geology and Palzontology at the Massachusetts Institute of Technology, Boston, for the remainder of the year. He succeeds Miss Elvira Wood who has gone to Washington, _D. C., on the U. S. Survey as assistant to Mr. Walcott. Dr. JAMes Furman Kemp, professor of geology in Co- lumbia University, delivered a lecture on “The discovery and development of mining districts,’ at Northwestern Univer- sity on Saturday evening, February 7th. The lecture was il- lustrated by lantern slides and was given under the auspices of the University Guild. GEOLOGICAL Society or WasHincron. At the meeting of this society on Wednesday, February 11th, the following program was presented: “Chitina copper deposits, Alaska,” W.C. Mendenhall; “An anthracite coal-field, three and one-half hours west of Washington,” David White; “The structure of a portion of South Mountain, Pennsylvania,’ George W. Stose; “Abandoned stream gaps in northern Washington,” Geo, Otis Smith. Tue CLayton Stone Axe. This is another axe from the loess, described by Dr. C. A. Peterson in Records of the Past for January, 1903, found at Clayton, near St. Louis, in the construction of a belt railroad. It lay at the bottom of the loess, fifteen feet below the surface, and has the form and ap- pearance of a neolithic instrument. The loess at that point lies on a tenacious red clay which may be the analogue of the geest underlying the loess at Lansing where the recent discov- ery was made of human remains. Tuomas Crowper CHAMBERLIN. On Saturday afternoon February 7th, a marble bust of professor Chamberlin. was presented to the University of Chicago by a number of his geological friends and admirers, chief among whom was pro- fessor J. C. Branner of Stanford University. In the absence of professor Branner the presentation of the bust to the Uni- versity was made by professor C. R. Van Hise of the Uni- versity of Wisconsin. A response was made by president William R. Harper of Chicago University, and remarks were made by Dr. H. Foster Bain and professor R. D. Salisbury. Letters were read from professor Samuel Calvin, Mr. Bailey Willis, professor H. L. Fairchild for the Geological Society of America, and Mr. S. F. Emmons. ; Tue American Museum of Natural History of New York city, has sent Dr. E. O. Hovey to the Lesser Antilles 194 The American Geologist. March 1. again, to supplement the studies which he made last summer on Martinique and St. Vincent. Dr. Hovey left New York by the steamer “Caribee” of the Quebec line on February 4th, and will remain in the Windward and Leeward islands two months or more. After studying the changes which have taken place on Martinique and St. Vincent as a result of the great eruptions which have occurred since last July, he will visit all the other important volcanic islands of the chain to photograph their craters, solfataras and boiling lakes, with the idea of making his final report upon the eruption of 1902 in the West Indies comprehend the entire series of Caribbean volcanoes. He will make collections of volcanic rocks and other materials for the Museum. A New Division oF THE UNITED STATES GEOLOGICAL SuRVEY. A new division, to be known as the division of hy- drology, has recently been organized in the hydrographic branch of the United States Geological Survey. The work of this division will include the gathering and filing of well re- cords of all kinds, the study of artesian and other problems relating to underground waters, and the investigation of the stratigraphy of the water-bearing and associated rocks. In addition to the gathering of statistics relating to the flow, cost, etc., of the wells, it is hoped in the future to give espec- ial attention to the geologic features which govern or which are related in any way to the supply of water. The division will be subdivided into two sections, the eastern and the western, the first embracing the Gulf and Mississippi River states and the states of the east, and the second embracing the remaining (‘‘reclamation’’) states and territories, or those having public lands. The charge of each section has been assigned to a geologist, the western section to Mr. N. H. Darton, and the eastern to Mr. M. L. Fuller. The office details are in charge of Mr. Fuller. The sections will be still further subdivided so that each state or group of adjacent states shall constitute a district in which the work of collecting data and of investigating the problems relating to underground water will be in charge of a geologist employed for the purpose. In the western section it is expected that the study of the geologic structure will be followed by the sinking of wells by the Survey, the aim being to test such of the arid or semi- arid regions as appear to present conditions favorable for ar- tesian water, with a view to their ultimate development for agricultural purposes. CHARLES MONROE HALL. THE AMERICAN GEOLOGIST, VoL. XXXI. PEATE culls Lee meee CE OLOGIST. Vout. XXXI. APRIL, 1903. No. 4. THE LIFE. AND WORK OF PROFESSOR CHARLES M. HALL. By WARREN UPHAM, St. Paul, Minn. PORTRAIT—PLATE XIII. In the comparatively new states west of Minnesota, resi- dent geologists are few. Many problems of theoretic and ec- onomic geology wait there to be worked out. The death of a young geologist, who was well equipped and earnest for this work, who had grown from boyhood to manhood in North Dakota, whom to know was to esteem and love, is therefore a great loss, not only to his personal friends, but to the wider interests of education and science. Charles Monroe Hall was born in Wellington, Ohio, Oc- tober 21, 1870. When he was about twelve years old, his par- ents and the family removed to North Dakota (then a part of Dakota Territory), settling in Stutsman county, near the pres- ent town of Eldridge. Later they removed to Grand Rapids, on the James river in La Moure county, where they engaged several years in farming. In 1891 his parents removed to the state of Virginia, where they have since resided,’ Charles, however, preferred to remain in North Dakota, entered the State Agricultural College at Fargo, went through the usual course of four years, and was graduated in 1895, with high honors. Immediately after his graduation, he was appointed assist- ant professor of chemistry and geology in that college, where he taught during the next two years. To better qualify him- self for his duties there, he then obtained a leave of absence for a year of special studies in Johns Hopkins University. 196 The American Geologist. ADE, oe Frederick Bennett Wright, his room-mate during this year at Baltimore, writes: “In the autumn of 1897 Mr. Hall en- tered the graduate department of geology. His enthusiasm in the work, together with his attractive personal character- istics, soon won for him a genuine popularity within the cir- cle of geological professors and students among whom he had come. Although his interest in the work before him was gen- eral, he was more attracted by structural and physiographic subjects than by those of mineralogy and paleontology. His life at Fargo, in the old bed of lake Agassiz, naturally gave him a keen interest also in glacial geology. During his stay at Johns Hopkins, he worked for a short time on the Mary- land Geological Survey, along the Potomac river. There his work was so thorough and satisfactory that he was offered a position in that state survey, for field work on the coastal plain the following summer. But his teaching and plans for field work in North Dakota were more attractive and caused him to return there. Personally he was very modest about his accomplishments, but yet had a sufficient sense of their 1m- portance to give him the confidence in himself necessary for success. I was greatly impressed with his broad views on all subjects, and his wide interest in general topics. We often had heated discussions, though perfectly friendly, which some- times lasted till after midnight, on all conceivable subjects, from geology, evolution, and theology, to music and, art.” Returning in the summer of 1898 to the Agricultural Col- lege of North Dakota, and being promoted to its professorship of geology, Hall was constantly engaged, through the remain- ing four and a half years of his life, in his duties as a college instructor, including frequent excursions with his classes, and in more extensive examinations of distant parts of the state during vacations. In the summer of 1900 he began a systematic investigation of the artesian wells and underground water resources of North Dakota, through co-operation by the Agricultural Col- lege with the United States Geological Survey. Previously also he had aided professor J. E. Todd, during one or two summers, on similar work in a part of the James river valley in South Dakota. Besides the hydrographic work, he began at the same time a survey of the soils of North Dakota, being associated with Charles M. Hall—Upham. 197 F. H. Newell and Milton Whitney, of the U. S. Geological Survey, in their respective departments of hydrology and soil investigations. Manuscript reports and maps, notes of stream measurements, records of artesian wells, collections and an- alyses of soils, etc., relating to parts of these researches already completed or well advanced, had been forwarded to Wash- ington, but they still await publication. Professor Hall had presented some of the results of this work in a series of newspaper articles, concerning the water supply of Fargo, the artesian basin and wells of the Red river valley and westward, irrigation for the drier western parts of the state, and the capabilities of its different regions for agriculture and grazing, these articles being published in the Fargo Forum and Daily Republican, the Wahpeton Gazette, the Minneapolis Journal, and other newspapers, during the years 1900 to 1902. One of the most important of these contributions is en- titled “A Discussion of the Water Resources of Fargo and Vicinity, with special consideration of possible sources of water for a better supply for the city,’ which filled four col- umns of the Forwm, June 24, 1902. It is accompanied with a section across the Red river valley, on the line of the Northern Pacific railway, and’a map which shows the limit of the chief artesian basin, receiving water from the Dakota sandstone, and the smaller areas of the valley receiving usually scantier flows from the drift deposits. Within the last month before his death, he completed a manuscript for the supplement in a school geography to be published by the American Book Company, this supplement being a “Geography of North Dakota.” Professor Hall represented his state through appointment by the governor, in the Tenth National Irrigation Congress, held at Colorado Springs, October 6 to 9 of last year; and in the Fargo Forum of November 22 he published a consider- able report of its proceedings, with earnest recommendation that North Dakota should take a larger share, in connection ‘ with the U. S. geological and hydrographical surveys, for the ,development of irrigation. The latest and perhaps the most important work which professor Hall brought to completion and publication, as print- ~- . 198 The American Geologist. setae es ot ed in December, 1902, is an “Official State Map and Prelimin- ary Geologic and Economic Map of North Dakota, issued by the Agricultural College Survey . . . in co-operation with the U.S. Geological Survey ; approved by Frank White, Gov- ernor of North Dakota, and R. J. Turner, Commissioner of Agriculture and Labor.” The scale of this map is seventeen miles to an inch. The western half of the state, and the Turtle mountains, are colored as Laramie clays and shales, with many outcrops and mines or openings of workable lignite. Thence eastward the remainder of the state, excepting the area of the glacial lake Agassiz, is colored as glacial drift overly- ing the Montana shales of Upper Cretaceous age. Upon these colors the courses of the marginal moraine belts are shown by another color printing. On the eastern border is the part of lake Agassiz west of the Red river, with its large Sheyenne, Elk Valley, and Pembina deltas. The extreme limit of the glacial drift, and the boundaries of the Dakota artesian basin, are designated approximately. October 22, 1901, professor Hall was married to Miss Jessie E. Taylor, of Fargo, and their life together was one of remarkable happiness and mutual helpfulness. They both were members of the First Methodist Episcopal church of Fargo, and of its choir. Professor Hall was also a member of the Masonic fraternity, the Knights Templar, and other social organizations. His last illness was diagnosed by physicians, half a year before he died, as probably to prove fatal within a year, or, at the longest, a few years. Yet he courageously continued his teaching and his plans for the state agricultural survey. One of his last pieces of work was to frame a legislative act giving to that survey, as aided by that of the United States, a distinct field not duplicating the work of the State Geolog- ical Survey, which is in progress under the auspices of the State University and School of Mines of North Dakota, at Grand Forks. His work of instruction in the college was continued until only three days before his death, which oc- curred at his home in Fargo the 22nd of January, 1903. For him is the divine promise, “Be thou faithful unto death, and I will give thee a crown of life.” ra Jaekel on Orthoceras—Ruedemann. 199 PROFESSOR JAEKEL’S THESES ON THE MODE OF EXISTENCE OF ORTHOCERAS AND OTHER CEPHALOPODS. By RUDOLF RUEDEMANN, Albany, N. Y. Professor Otto Jaekel presented at the February (1902) meeting of the Deutsche Geologische Gesellschaft the follow- ing theses, which were discussed at the March meeting and at a special meeting in April.* “1. We should not conceive of the orthoceratites as free- swimming organisms, but, like the colularias, actually sessile in such a fashion that their chambered shell grew upward from a bell-shaped fixed embryo-chamber and throughout life re- tained flexible connection with this by means of .conchioline secretions. “2. The formation of septa and camere served, as in corals, Hippurites and some sessile, erect gastropods, to lift the body above the sea bottom (growing upward by. sedimentation), without necessitating an essential alteration of its form, and also to facilitate the upright posture of the shell and its animal on a relatively small base. “3. The siphonal cord then appears to be that portion of the body which is reduced by the formation of camerze. As com- pared with other animals bearing chambered shells its form- ation becomes intelligible by the fact that the body grows only secondarily from the original fixation or embryonal chamber, and that the latter was hence an integral part of the original body. “4. The siphonal calcareous secretions (obstructive rings and endosiphonal calcareous deposits in the lowermost part of the shell of the endoceratites) serve to ballast the body so as to counterbalance the formation of air chambers, which latter guarantee an upright position. “s. The involute Nautiloidea in the restricted meaning, have discarded fixation, either from the beginning or in later stages of their development. Their protoconch consisted of conchiolin and was therefore not capable of preservation. For this reason, it cannot be determined whether it was retained by * Published in Zeitschr. der Deutschen Geol. Gesellsch, 54 Bd., 1902, p. 67- 101. 200 The American Geologist. es the animal on the shell or whether the chambered portion of the shell parted from the protoconch. Both cases are possible, the former more probable. I have seen its oval impression on the succeeding volution of a Nautilus barrandei from the al- pine Keuper. The first chamber of the Nautiloidea is hence not the protoconch, but the first air-chamber, which at the low- er end shows a scar for the passage of the siphuncle from the protoconch into the chambered portion of the shell like that in the orthoceratites. “6, The semi-involute Nautiloidea, the cyrtoceratites in a broad sense, are not transitional types from the orthoceratites to the involute Nautiloidea, but regressive types of the latter. The involution in every case presupposes a free state of the individual, hence at least an early detachment if not an absence of attachment. “7 The forms with contracted ostium or aperture, as Gomphoceras, Phragmoceras, Tetrameroceras, Hexameroceras, were probably imbedded in the silt with their entire shell and protruded only their arms and their funnel, which here as in other mollusks was a sipho, 1.e. a breathing tube. “8 The ammonites and belemnites were free from their inception, as they have retained their embryo-chamber in form of a calcareous ovoid bulb on their chambered shells. “g. The rostrum of the belemnites was not a rostrum, ie. a water-cutter, but a parillus, a post to be driven into the ground; the belemnites were hence not free and, as generally supposed, rapidly swimming, but were sedentary animals. “to. The higher ‘“Dibranchiates,’ the ink-fishes proper, have become crawlers or have acquired a retrograde swim- ming motion by means of the funnel. With the exception of the cuttle-fishes, which developed from the belemnites and which, in Spirulirostra and Spirula, show interesting regres- sive characters, the skeleton of the remaining dibranchiates, is reduced either completely in the benthonic, essentially creeping octopods, or has, after complete obliteration of the “rostrum,” become a flexible axial support, which consists of conchiolin and is comparable to the vertebral column, in the slender Oigopside which became better swimmers and possess even paired terminal fins. Jaekel on Orthoceras—Ruedemann. 201 I beg to add the following theses on the relation of the cephalopod to the other mollusks : “tr. I consider as progenitors or as proseries of the cephalopods, the conularias, in which the body form and shell secretion of the orthocetatites was inaugurated and the form- ation of four gills, which it would be difficu't to derive from the body form of the cephalopods, was established. Lateral members of this proseries we find in the Hyolithidz, which present in their incomplete formation of septa and the well developed formation of opercles, certain analogies to the ceph- alopods. (The aptychi are herein considered as cuticular calcifications of the hood, which in Nautilus serves for ex- ternal closure of the ostium, )” Professor Jaekel made some general remarks on the form and purpose of these theses from which we learn that the form in which they are presented is simply to invite discussion, This appeared necessary because the biological consideration of these extinct mollusks has gradually fallen too far behind their morphologic and systematic treatment, and it can be hardly dis- puted that with such aberrant types as the orthoceratites and belemnites an understanding of their organization can be at- tained only by thorough consideration of their mode of life. As the meaning of changes in organs can be ascertained only in a biologic way, and while the paleontologist has perpetually to deal with processes of alteration, there is also in this field the necessity of the biologic mode. In explanation of theses 1 and 4, which refer to the organ- ization of the orthoceratites, we find the following remarks: “With the view hitherto current that the orthoceratites moved through the water like the slender squids of the pres- ent (Oigopsidz), that hence the apex of the orthoceracone was directed forward when in motion and served as a water-cutter, the following parts of their organization seem to me to be spec- ially at variance: “a) The calcareous shell of the orthoceratites is much too thick and heavy for a pelagic habit, moreover it is in some forms often loaded with special calcareous secretions. “b) The external sculpture of the shell excludes the possi- bility that the latter could have been imbedded in the flesh of the body; hence active swimming organs could protrude only at the apertural end of the shell (ostium). 202 The American Geologist. DEEL ae “c) The shell not only frequently shows a pronounced transverse sculpture, but it may even be provided with ring- like swellings (annulate forms). Both phenomena are irrecon- cilable with a rostral function of the shell, as both would offer friction and resistance to the water pressure. “d) The strictly symmetrical form of the shell contrasts sharply with the shells of the squids, nor does it, aside from its heaviness, find an analog in the shell form of the pteropods, which also fail to display any such pronounced monaxial bi- lateral symmetry. “e) The straight truncation of the ostial margin, together with the symmetrical form of the whole shell, excludes also the possibility that the orthoceratites were crawlers bearing their shells on their backs after the fashion of snails. “On the other hand, the following facts argue, in my opin- ion, for the sessility of the orthoceratites : ' “a) The radially symmetric structure, which everywhere in the animal kingdom is characteristic of sessile forms, ap- pears in the circular section, the straight truncation of the aperture of typical orthoceratites, the position of the three or five submarginal impressions in the living chamber, the regu- lar growth in thickness and an occasional regular, radially symmetric arrangement of longitudinal ridges upon the sur- face, and can be readily explained only by conditions of static pressure during growth. “b) The shell is usually broken off at its lower end; which is an exceptional condition in externally similar gastropod shells such as Fusus, Turritella, Terebra or in the very slender shells of pteropods. Among the thousands of observed orthocera- cones initial chambers have become known in but a few forms. The apex is hence nearly always broken, a fact which indicates that it was held by an external force after the death of the animal. In those cases where the apex has been observed in well preserved state, it shows a scar which, like that at the first air chamber of the ammonites, apparently permitted to the sipho a connection with the contents of a protoconch as yet unknown. “c) The agreement of the shell structure of the orthoce- ratites with the conularias seems to me unmistakable. The latter show a radially symmetric structure; with them a trans- Jackel on Orthoceras.—Ruedemann. 203 verse sculpture predominates; among them the apex is com- monly broken off; further their pronounced tetramery appears to me to throw light upon some hitherto unexplained facts of the organization of the cephalopods, such as the possession of four gills among the older cephalopods, a condition which, as is well known, is eventually lost in this class and yields to dibranchy ; and further, upon the remarkable tetramerous cell division of the cephalopod embryos. While we have until lately, been without any clew to the mode of life of the con- ularias and from the external similarity of the shell with that of certain pteropods have inferred a pelagic habit for these organisms, Ruedemann in Albany, U. S., has made a discov- ery, which is most interesting, though little noticed in liter- ature, namely a colony of young conularias fastened by a rel- atively large, conically attached basal chamber to the sea bot- tom or to other objects. (R.Ruedemann. The discovery of a sessile Conularia 15th Ann. Rept. of the N. Y. State Geolo- gist. Preliminary partial reports in the AMERICAN GEOLO- Gist coo, XV1i~-p. 1583 xviliP p. 65.) “Proceeding from certain ideas stated by A. E. Verrill (Amer. Jour. of Science, 1896, v. 2. p. 80) Ruedemann has ‘briefly expressed the opinion that the conularias might be the ancestors of the cephalopods. To the probable objection that, in distinction to the calci-testaceous cephalopods, the conular- ias possessed a chitinous skeleton, he points to Chrondro- phora with its chitinous skeleton and states in accordance with the views of Hyatt and others, that the initial chamber of var- ious nautiloids might have been chitinous. In regard to this I would remark, that, in my opinion, the shell of the conularias did not consist of chitin, but of conchiolin and hence was in principle like that of the molusks. Moreover, [as stated by Ruedemann,]| we find in various phyla of the animal kingdom, as Anthozoa, Bryozoa, Brachiopoda, that so-called horny skel- etons precede the calcareous. “Ruedemann holds the view that the conularias were ses- sile only in their youth and later became free, or at least could quite likely be so. The acceptation of such a possibility seems to me to be essentially a concession to the old view concern- ing these forms, and has probably not been confirmed since. Besides, this assumption would be opposed by nearly the same 204 The American Geologist. een a ee considerations as the free mobility of the orthoceratites. But as here the fixation of younger individuals and of very difter- ent sizes, has been proved, and no fact in the shell structure of mature conularias points to other biologic relations, we are not only justified but bound to assume also a fixation of the ma- ture conularias until the contrary has been demonstrated. From the Upper Siluric of Ludlow in England (Lower Lud- low beds) I have collected a conularia having a hight of ca seventy cm. and hence surely to be considered as fully grown, and which, at its pointed end, shows, corresponding to some growth-stages figured by Ruedemann, such striking phenom- ena of bagging in its growth, that I believe I am justified in citing it as a direct argument for persisting sessility. “d) A transverse cameration of a shell, i.e. in its primitive form, an advancing in the shell by means of the formation of septa, is found without exception among sessile organisms,* not only as a typical character of certain groups of life forms, as the corals, Chetetidae Sphinctozoa, but also singly in other divisions and specially such as, in contrast to their relatives, combine attachment with vertical growth, such as Richthofenia among the brachiopods, Hippurites among the bivalves, Ver- metus among the gastropods. Such cases as these make cam- eration appear as a result of vertical sessility and therefore al- low us to infer from such cameration, this sessile mode of life. “Under the former mode of construing the orthoceratites it would have been difficult to cite any probable reason for the cameration. On the contrary it would be very strange if just that part of the shell had been rendered most fragile by the formation of air-chambers, if in swimming it would, as ros- trum, have had to possess.the greatest power of resistance. “Of special moment is the consideration that the formation of air-chambers may have largely diminished the body weight of the orthoceratites and thereby have counterbalanced the pressure which otherwise would have rested upon the apex of the shell. The latter was thereby largely strained by an up- ward pull at the basal chamber and under these circumstances the structure could hardly have been more advantage- ***The chambered calcareous foraminifers can not here be used for biologic comparison, as all chambers are filled with protoplasm and cameration does not involve a separation of the animal from the posteriorly situated cham- bers.”’ Jaekel on Orthoceras.—Ruedemann. 205 ous. For the fixation at one point allows a balancing move- ment in all directions and may be conceived to have been af- fected by vertically stretched ligaments, which, ring-like, em- brace the initial shell. The orthogenetic* formation of the chambers exerts an increasing pull upon the chamber of at- tachment, and as a completed structure, by the law of accelera- tion, appears in successively earlier stages of the ontogeny, it is obvious that cameration finally led to detachment among a part of the forms. “e) The siphonal cord which has always been the most peculiar enigma in the cephalopod organization, has found very different interpretations, but none of these has been ac- cepted as wholly satisfactory. It can hardly be considered as an organ of fixation for the shell, because, on one hand the animal is held in the living chamber by a muscle of attach- ment, and on the other hand the siphuncle in Nautilus has by no means the histologic character of a ligament, and finally it would remain unintelligible why it then perforates the whole shell throughout lifetime and is not concentrated upon the last septal wall. “If we now proceed from the idea that the chambered cep- halopod shell originated from a sessile protcconch, the forma- tion of the siphuncle appears at once in quite different light. The siphuncle is then nothing but a portion of the body restricted by ihe formation of the chambers. It becomes biologically analogous to the wmbilical cord of the mammals, more specially however to that portion of the pelmatozoans, which is con- stricted by the stem joints, and these analogies appear also for that reason to be not without meaning, for various facts point to phylogenetic relations of these types. I will hereby exclude at once the supposition that I would derive the vertebrates from the cephalopods or pelmatozoans, on the contrary, in my opinion, some facts seem to argue for a derivation of the mollusks as well as of the echinoderms from higher types of the group of the episomatides by repression of development (O. Jaekel. Uber die Stammform der Wirbeltiere; Sitz.-Ber. Ges. naturforsch. Freunde, Berlin, 1896, S. 116). “According to this view the siphonal cord would enclose a portion of the somatic cavity, which kept the embryonic body *O. JAEKEL. Ueber verschiedene Wege phylogenetischer Entwicklung. GUST.’ FISCHER. Jena. 1902. 206 The American Geologist. a ieee in connection with the definitive body. The analogy with the crinoid stem extends further also on genetic and histologic relations. In both the tubes are wide in the older forms and become more and more constricted in the later by expulsion of the intestines. . . . In older crinoids with wide stems, the cord must have enclosed a considerable portion of the somatic cavity and have been in connection with the root, but in later forms this whole portion has been reduced to a fibrous tissue that no longer shows distinct processes of differentiation and therefore has been differently interpreted (Comp. Jaekel in Stammesgeschichte der Pelmatozoen, I, 1890, p. 77-79). “Very similar are the special conditions of the formation of the siphuncle. In the older forms it is frequently very wide; with the later it is mostly narrow, and it becomes finally rudi- mentary when the shell was never attached. “The remarkable expansions of the siphonal tube of or- thoceratites, which hitherto could not be accounted for, would now appear to find their explanation in the supposition, that a constriction of the air-chamber would increase the weight and thereby the stability of the shell upon the bottom. The siphon- al calcareous secretions would also have to be regarded as for the same purpose.” Our space does not permit us to reproduce here the auth- or’s explanatory remarks of his theses 5 and 6, but we con- sider the views presented on behalf of thesis 7 so suggestive that we cite them in part: “To thesis 7, referring to the contraction of the ostium of various nautiloids, as in Gomphoceras, Phragmoceras, Tetra- meroceras and Hexameroceras, I desire to add the following explanation: To begin with, it cannot be doubted that accord- ing to the current view the single median sinus [of the aper- ture] corresponds to the position of the funnel, and that the paired symmetric sinuses of the infolded upper shell-margin embraced the arm bases and that hence the mouth lay between them. These are the only fossil ammonoids which give some clew to the form of the cephalosoma and specially to the po- sition of the arms on the head, but which still have been little considered in this connection. The interest in these ostial forms is still hightened by the fact that of nearly related forms, such as Tetrameroceras, Hexameroceras, Octomeroceras, the Jaekel on Orthoceras—Ruedemann. 207 one possesses four, another six, the third eight, Phragmoceras .and Gomphoceras however but two sinuses, which obviously denote separate arms. One conceives, now, the development of the arms usually thus; that in nautiloids numerous arms were present in indefinite number, and that the latter consol- idated in the younger types to ten (decapods) and to eight (octopods). It is however, according to the ontogenetic de- velopment of the arms of the living dibranchiates and the mor- phologic arrangement of the so-called head tentacles of Nau- tilus, much more probable that the latter are but evaginations of the arms, which quite likely do not correspond to the single arms of other cephalopods. “Hexameroceras osiliense shows on either side three arms sinuses which gradually increase in size upward from the fun- nel sinus. The figure presented by their arrangement may be directly compared with growth-stages of living dibranchiates. While in the mature sepia the arms surround the mouth radially, their inception is a paired one with a distinct sym- metry, so that with the appearance of the last arms the mouth becomes surrounded and enclosed by the circle of arms. Two pairs are developed first and these are soon followed by the third. These three pairs may also here be indicated and in the case cited may have flanked the mouth laterally. The encirc- ling of the mouth, which ontogenetically takes place at a late stage, had here not yet been accomplished. The circle is in- terrupted by a hood, partly overhanging the mouth as in Nau- tilus, in which however the formation of the arms has been spec- ialized in quite different direction from that of these Siluric types. In the oral view of Nautilus one sees what can not be learned from the current representation of the animal, namely that the mouth in the center is flanked on both sides by three leaf-like compressed arms, which are provided with muscular, contractile, transversely striated tentacles. As to their ontogenetic succession of position we know un- fortunately nothing and one must consider the exterior and strongest as homologous to the first arm of the dibranchiates, the inner ones as the second and third pairs, which are more distant from the funnel. . . . We can not conclude that in these forms the funnel was, in contrast to Nautilus, open upon the oral side simply from the fact that [in Hexameroceras, 208 The American Geologist. One eS ee etc.| the shell parts approaching each other above the funnel leave a slit open between them. Its inception in all dibranch- lates argues for the secondary coalescence of the walls. There is on the whole little probability that a funnel like that of Nau- tilus was placed under this slit; we will hardly be amiss if we locate the arms in the aperture which is directed aborally baeck- ward. The funnel in the typical form of a folded muscle-plate, as it 1s found persistently in Nautilus and embryonally in the dibranchiates, or in the specialized form of a distally circular, coalescent tube, as in the mature dibranchiates, presents prob- ably specialized conditions adapted to the peculiar mode of movement of free living cephalopods. I consider it probable that the arms of these older nautiloids were spread out blade- like and, as in Nautilus, provided with erectile tentacles. The contracted aperture of several ammonites appears so similar to that of the gomphoceratites, that one may at least infer blade- or spathe-like arms. “The activity of these forms can hardly have been very great or comparable in any way to that of recent dibranchiates. The advanced closure of the shell suggests the balanides and lepadides, the bryozoans and various types of worms as serpu- lites, and seems, therefore to suggest the probability that these for genera mentioned (Hexameroceras etc.) were sessile. -The manner in which the shell conformed itself to the arm-bases appears most easily explained as a special provision for pre- venting ‘an intrusion of foreign bodies between mantle and shell. This fact, pointing to a strong dependence upon the bottom, together with the bilaterally symmetric form of the shell, has led me to the supposition that these animals lay im- bedded vertically (hence symmetrically) in the bottom of the sea and spread out their arms upon it. The strong projection of the funnel-sinus would also be explained by this supposition, as it then would have had to exercise the function of a real siphuncle. To colleagues, to whom this explanation may ap- pear strange and bold, I wish to point out that some Spatan- gide lie buried about a foot deep in the sea bottom, protrude their long tentacles through a tube, and through another dis- charge, by energetic water current, the contents of their intes- tine. Here one has, therefore, quite analogous conditions, which would have hardly been expected from an echinid. Jackel on Orthoceras—Ruedemann. 209 “Tt also seems important to me to recall here the fact that not only the living octopods, but also decapods like Sepia, hide in manifold ways upon or in the bottom, either by piling up stones and other foreign bodies upon them, or by stirring up with their fins so much sand that their back becomes entire- ly hidden. From such conditions to the supposed mode of ex- istence of the phragmoceratites, there seems to me only a short step. The firm attachment of Spirula at the bottom will, in this connection, find an explanation as a phenomenon of re- gression.” We omit here the remarks upon theses 8-10, interesting as they may be, as they refer to belemnites and younger dibranch- jates, and are somewhat remote from the major propositions of the author. The discussion which followed professor Jaekel’s remarks was, judging from the record, both animated and instructive. Space forbids me to give more than meagre notes of the argu- ments and objections made. Professor Branco pointed out that orthoceratites, belemnites and gomphoceratites are never found in a vertical or erect position, while professor Beus- hausen mentioned the occurrence of long orthoceratites in vertical position in the Oneonta sandstone of New York, an occurrence made known by professor Clarke. (N. Y. Siate Mus. bull. No. 39, 1900, pp. 167-171.) Others found it diffi- cult to understand how endoceratites often several meters long could have been supported upon a delicate apex and that the bases had never been found in sediments, such as clay, where all firm tissues are as a rule excellently preserved. These arguments were met by the declaration, that firm ligaments held the lower part of the shell upon the bgsis, that the vertical position of the shell was essentially effected by the air cham- bers and that the latter, after the death of the animal and the decay of the basal tissues may have drawn the shells away from the bases. Specially interesting were the remarks of professor vy. Mar- tens, whose experience as biologist enabled him to illuminate from various sides the problem of the mode of existence of Orthoceras. V. Martens agrees with Jaekel in that the ortho- ceratites were not free-swimming or pelagic animals, as these have all extremely thin, fragile shells and are, in all classes of 210 The American Geologist. pri aa the animal kingdom, bilateral, like a ship. If Orthoceras lived at the bottom it could have moved along as Sepia does,—the long conical shell is no proof of the contrary, as such gastro- pods as Cerithium and Turritella demonstrate. But it must then have had strong motive organs, directed toward the bot- tom, and if the shell was external, one would not expect to find an apertural plane vertical to the axis of the shell as in Orthoceras, but inclining toward the ventral side of the ani- mal, as in the gastropods mentioned; if the shell were whol- ly internal, or at least on its anterior part, then it would, as in Sepia, adapt itself to the bilateral form of the animal, which in its turn adapts itself to the surface of the sea bottom. A conical, cylindrical or sack-shaped body with decided differ- entiation of both ends and uniformity in circumference is the characteristic form for animals of little motion, in which the upper and anterior ends are identical, i.e. for sessile forms, as certain infusorians, corals, crinoids, ascidians and cirripeds. A decided approach to this body form is, among the living cephalopods, found in Octopus, which prefers to sit in cavities of the rocky bottom and to extend thence his arms in all di- rections in search of prey. Mr. v. Martens stated further that the strong development of the calcareous shell in Orthoceras certainly argued for a very early sessility in the development of the young Orthoceras. The base of attachment may, as in Fungide and oysters, have been a very small stone or snail shell; the smallness of which may have forced the older ortho- ceratite to effect its static support by sinking its lower end into the soft mud. Finally it was pointed out by the same investigator that one must not be afr@id to assume within a class of quite uni- form internal organization, a very great variety in the exterior mode of existence; the great difference in the external appear- ance indicates this distinctly, and it is actually found in many classes of animals, as among the gastropods, which are most closely related to the cephalopods, and also among the lamel- libranchs. We hope that these theses will be taken as such by Ameri- can paleontologists, i.e. as challenges to a discussion of the biologic relations of the groups involved; and of the orthocer- atites in particular. There is no doubt that such a discussion Jaekel on Orthoceras—Ruedemann. 211 will aid in rendering our conception of these forms more con- cise by bringing out observations stored up in the notes of in- vestigators. With this purpose this translation has been pre- pared and the present writer desires to add a few annotations to these significant contentions. It has been asserted on various excellent grounds that life originated in the coastal regions with benthonic forms; that slowly creeping organisms preceded the planktonic and nektonic forms in the lower phyla of the animal kingdom. This principle may, in its totality, be well applied to the Cephalopoda, for here all the living forms are mostly rapid movers in contrast to the evidently sluggish forms with heavy shells, belonging to the early geologic per- iods. In the Mesozoic we find the ammonoids, which for good reason, are now considered as bottom crawlers; and as we go back in time in the paleozoic we find the coiled forms largely replaced by the orthoceracones. Notwithstanding the fact that Barrande demonstrated that the whole series of forms from the straight to the involute nautiloids was present in the earliest period, and the declaration of Jaekel (in explanation of thesis 6) that the slightly curved forms are not transitional between the involute nautiloids and the orthoceracones, but are types of repression of development of the former, and that, further, the majority of these faintly involute forms do not appear until Upper Siluric and Devonic time, it can be statistically estab- lished, as Hyatt affirms, “that the straight cones predominate in the Silurian and earlier periods; while the loosely coiled are much less numerous, and the close coiled and involute, though present, are also rare.”” We cite here Hyatt’s lucid exposition of these facts (Phylogeny of an Acquired Characteristic. p. 300) : “But suppose we reverse the course of nature and follow back the diminishing number of nautilian and gyroceran shells. We then see, upon arriving at the Silurian, that the vanishing point of these shells, although not traceable on account of the lost records of Protozoic time, could not have been far distant, while the increasing number and varied forms of the straight cones indicates for them a more remote focus in time and con- sequently a more ancient origin. Thus we are able to see that, antecedent to the Silurian, in the Protozoic, there must have 212 The American Geologist. April, 1903. been a time when the straight cones or their immediate an- cestors predominated, to the exclusion of the coiled and per- haps even of the arcuate types.” If now the orthoceratites were actually the earliest cephal- opods we may, by application of the general principle regard- ing the origin of life, mentioned above, infer that they were certainly not free swimming forms, but either sluggish crawl- ers or wholly sessile. As the structure of their shells would seem to exclude the crawling habit, the sessile would remain by exclusion. d On the other hand, it can not be denied that facts present themselves which do not corroborate the theory of the sessile mode of life of Orthoceras. It becomes evident from Jaekel’s remarks and explanations that the presence of “‘air-chambers”’ is considered necessary to relieve the apex of the shell from the weight of the shell and animal by the upward pressure of the contained air. The current view is thereby retained that ° the chambers of the cephalopod shells were “air-chambers ” This view seems, however, by no means established, for Verrill (see Zittel-Eastman. Text book of Palentology, p. 508) states that the chambers of Nautilus stand by way of the siphuncle and pericardium in direct connection with the gill cavity, and adds: “Thus sea-water can readily pass into or out from the chambers of the shell, to equalize pressure at varying depths, as in most marine Mollusca. These chambers are unquestion- ably filled with fluid under normal conditions. But living as the animal does under pressure at considerable depths, the fluid in the chambers is saturated with the gases in solution. When the Nautilus is rapidly brought to the surface, some of the gas is liberated in consequence of diminished pressure, and must occupy part of the space within the chambers by forcing out some of the fluid. Hence the shell will float until the free gases within the chambers are absorbed or otherwise eliminated. There is no evidence that free gases are ever naturally present in the living chambers during life.” If the living Nautilus has its chambers filled with water, the inference is that the extinct cephalopods had it likewise. Hyatt has therefore properly proposed the non-committal term “camere” for the compartments of the cephalopod shell. The fact of the filling of the chambers with water would, however, Jaekel on Orthoceras—Ruedemann. 213 considerably alter the conditions of static pressure of the orth- oceran shell. The calcareous siphonal excretions would then have hardly been intended to counterbalance the upward pull of the air-chambers and to furnish stability to the conch, they would rather appear to have increased the evil of pressure upon the apex. Of special interest in this connection is the endoceratite, Nanno aulema Clarke, from the Trenton of Minnesota (Geol. Surv. Minn. v. 3, pt. 2; Pal. p. 770). This cephalopod had a wide proseptal siphonal cone, which is filled with solid lime- stone, a modification of the original organic deposit. This solid, heavy apical cone was “unquestionably,” as Clarke as- serts, “external except so far as ensheathed by a mere ccat- ing or film of the shell-tube.” The chambered portion of the shell includes only a few relatively small chambers. This animal must have undoubtedly iived like the belemnites, and the apical cone must be functionally analogous to the rostrum of the latter. In regard to the belemnites it is claimed by Hyatt and still more definitely by Jaekel, that they buried themselves in the mud and used the rostrum as a post, “‘pax- illus,” as Jaekel terms it, to secure themselves in the soft ground. We have then in Nanno an orthoceratite of which we can claim that it followed the same praxis. This, how- ever, gives us a hint as to the use of the heavy deposits in the siphuncle of the other endoceratites, as well as of Actinoceras, Hormoceras and the groups of species of Orthoceras, occur- ring in the Deyonic Schoharie grit of New York. The most typical of these Schoharie grit species, Orthoceras luxum, prav- um and oppletum frequently have their entire chambers solidly filled with organic deposits as examination of the plates of the New York Paleontology, v. 5, pt. 2, (f. i. pl. 81) will readily show. It is a very suggestive fact that this Schoharie grit is a sediment consisting of quartz sand in a limestone matrix, which by its composition and enclosed fauna indicates deposi- tion in the littoral zone and in disturbed waters. It seems prob- able that these orthoceratites used the weight of their shells to anchor themselves in the sand and thus prevent their being torn from their moorings. But if these orthoceratites buried themselves in the ground, it is very probable that all the others did the same. 214 The American Geologist. April, 1908: In this connection, it is still further to be considered that endoceratites of the Trenton attained a length of six- teen feet or more. While it is already difficult to under- stand how these giants could have balanced themselves upon their apex, it would appear still more unintelligible that they should have striven to raise themselves so high above the sea bottom when their recent descendants find it so much more advantageous to lie low in the mud and to prey upon the much richer fauna of the vagile benthos. Besides, in the Trenton period, the fish-fauna was certainly small and the majority of all organisms, which we have from that period, were still bot- tom-crawlers. These considerations suggest to me the sup- position, that the orthoconic cephalopods may have fixed themselves only in their youth to small objects, to gain a foot- hold, as professor v. Martens suggested, but later on may have allowed themselves to sink, or actively worked themselves into the ooze and perhaps also may have piled sediments around them, in order to gain steadiness and to hide them- selves.- The occurrence of numerous upright orthoceratites in the Oneonta beds of New York also mentioned in the discus- sion of the theses, may serve to support this view, in case it can be proved that the orthoceratites were killed in situ by an inflow of fresh water, as is indicated by the presence of Am- nigenias. The objection that no other orthoceratites, with the excep- tion of those just mentioned, are found in vertical position in the sediments, is probably to be met by the observation that the shells of the recent Nautilus, which is a bottom-crawler, and even those of the Spirula which lives sessile at considerable depth, rise after the death of the animals to the surface and become pseudo-planktonic, a fact fully established by Walther (Zeitschrift der Deutsch. Geol. Gesellsch., 1897, 49: 258). The cause of this phenomenon, if the chamber during life time of the animal were filled with water, is not quite apparent, but perhaps is to be sought in the decay of the organic tissues; and it is to be inferred that the same took place with the ex- tinct cephalopods and to some extent also with the shells of Orthoceras. ‘The writer has seen exposed near Valcour, Lake Champlain, on large surfaces of Beekmantown limestone, which were clearly shore-deposits of that period, the tangled growth Jaekel on Orthoceras—Ruedemann. 215 of sea-weeds, between which run, in approximately east-west- erly direction, narrow tide channels filled with black mud and a rich mass of gastropods and large straight cephalopod shells, The latter lay parallel to the direction of the channel and were clearly wedged in or drifted in together with the gastropods, which often lay piled up behind the Orthoceras shells. There is further to be accounted for the existence of forms like Orthoceras truncatus Miinster. This was in the habit of regularly breaking off the cone of its shell and then mending the mutilated apex with a plug. It can not have been sessile, but as the crawling, more or less involute forms are supposed to have developed from the sessile orthoceratites it must be conceded that these truncate orthoceratites were possibly forms which had finally taken the step of detaching themselves but instead of rolling up, discarded the unwieldy cones. The slight- ly curved Oncoceratites probably stand in close connection to these forms and are the result of further adaptation to the crawling mode of life. At the same time appears the fact that these species preferred to discard entirely the greater part of the conch instead of rolling it up, to argue for the supposition that the camer were of little or in fact of no use as hydro- static apparatus and indeed but a hindrance to movement. Our supposition that the orthoceratites may probably have planted themselves in the oceanic deposits, does not appear to agree well with Jaekel’s conclusion that this was the mode of existence of nautiloids with contracted apertures as Gomphoc- eras and Phragmoceras, as the latter with their breviconic, rapidly expanding cones would seem to have adapted them- selves to an entirely different habit of life as the orthoceratites. But it is here to be considered that the breviconic form of the shells may well have been the result of further complication of their structure as Dr. Clarke suggested to me, namely of the contraction of the aperture, which invited a lateral expansion of the animal, thus producing low and broad living chambers and camerz. Furthermore the broad low shell of these forms is obviously well adapted to squatting upon the sea bottom. From the contraction of the aperture and the resulting con- striction of the arm-bases, Hyatt concludes that the arms could not have been powerful enough in these forms for a crawling habit and that they hence were either sessile or swimming. 216 The American Geologist. oes The strong constriction of the aperture, which points to forms - like Lepadidze and, Balanidz, combats the latter possibility. Sessility remains then alone the alternative. In regard to this habit I would like to add that our considerable New York fauna suggests the occurrence of two different methods of ses- sility of these organisms. We have, on one hand the rather large turbinate types of Gomphoceras, which find their princi- pal development in the Schoharie grit, Hamilton shale and also in the Gontatite limestone. These clearly give the impression of having been planted vertically in the mud with their apical portions, the expanded portion resting on the surface of the bottom. On the other hand, however, we have lately be- come acquainted with a relatively rich fauna of small, slightly _curved, in general talon-like types of Poterioceras in the Guelph beds of New York, and similar forms are known from the Chazy and Trenton limestones. These are obtained from beds which are coralligenous. They are characterized by their relatively small size, their tendency to assume curved and bi- lateral symmetric shape, and above all, the fact of their fre- quently discarding or losing the greater part of the conch, so that only a few of the last camerze are found adhering to the living chamber. These peculiarities appear to point to a differ- ent mode of life and, in connection with their occurrence in the coralligenous beds, suggest that they may have lived in the cavities of the reefs themselves, just as living cephalopods hide themselves in rocky caves. ANNOTATIONS. By JOHN M. CLARKE. Essential to professor Jaekel’s conception of fixation in Orthoceras, seems to be the assumption of a conchiolin proto- conch. The existence of this structure in such form can not be regarded as demonstrated. Professor Hyatt was not pre- pared even after a close study of the putative calcified Orthoc- eras protoconch described by the writer, to grant that it apper- tained to that genus. Confirmatory evidence was at that time lacking,—it was the only recorded instance of an Orthoceras- like shell in which the protoconch was retained, and the object could not be generically interpreted from its intrinsic char- acters. The presumption, in view of the examples brought mo Jaekel on Orthoceras—Ruedemann. 217 forward by Barrande and Hyatt in which only a cicatrix was shown, was against its orthoceran character. The writer's in- terpretation of it, however, finds corroboration now in the recent discovery by Pocta of many young~ ortho¢eran shells bearing calcified protoconchs. Whether we regard the genus Bactrites as nautiloid or ammonoid, it is a longicone like Or- thoceras and that it had a well developed, fully calcified pro- toconch, has been abundantly shown (Branco, the writer), in- deed specimens with protoconch attached are no longer uncom- mon occurrences. Whatever mode of life is postulated of Or- thoceras must be equally true of Bactrites and it is clear that the latter could never have been fixed at its apex. A calcified protoconch at once demolishes the strange structure with which Jaekel would prop up the Orthoceras. I am disposed to be- lieve there is reason to infer that while in early and primitive forms of Orthoceras the protoconch may have been wholly of conchiolin, in later forms, through acceleration or other causes, calcification might have set in at an initial stage. The suggestion that Orthoceras buried itself vertically in the mud, impresses me as intelligible and helpful; that it was affixed at the sea- bottom seems unessential and unlikely. As the occurrence of vertical Orthoceras in the Oneonta sandstone at Oxford, N. Y., which has been twice referred to in the foregoing, constitutes the only observed illustration of the presumed normal attitude of these shells, I may say that the interpretation suggested by Dr. Ruedemann is in approx- imate agreement with the other conditions wherewith the occurrence is involved. ‘These bodies are highly abundant in a certain stratum, which lies at the outer edge of a Devonic fresh or brackish water lagoon where land drainage was re- ceived in great quantity. An excessive outflow at time of freshet, carrying the fresh waters beyond their proper bound- ary, probably would have killed outright a settlement of Or- thoceras buried in the littoral muds without, and have washed into close proximity to them remains of Amnigenia and terres- trial plants such as characterize the true Oneonta deposits. Whether such an outflow could have swept away from the Orthoceras settlement all mobile forms of marine life may be a question for determination, but it is true that as yet no other trace of marine life has been found in this bed. 218 The American Geologist. April 306. THE CENTRAL OHIO NATURAL GAS FIELDS.* By J. A. BOWNOCKER, Columbus, O. PLATE XIV. Introduction. Four fairly distinct reservoirs of gas have been discovered in central Ohio. Geographically, however, they are closely re- lated, and the same is true geologically, and for these reasons all will be considered together. In other words the several reservoirs will be regarded merely as parts of one large field. Locations and Areas. At the present time the gas fields consist of two parts, one known as Sugar Grove, and the other as Homer. Between .these, two additional reservoirs have been discovered, but both have long been exhausted; one lay at Thurston, Eairfield county, and the other around Newark, Licking county. By far the most important reservoir is in Fairfield and Hocking counties and is known as the Sugar Grove. It in- cludes parts of the following townships in Fairfield—Berne, Pleasant, Rush Creek and Madison, but in the last two, how- ever, very few wells are found. In Hocking county lying south of Fairfield, the producing territory includes parts of Good Hope, Laurel, and Marion townships. The length of this field as developed in 1902 was sixteen miles, and the max- imum width eleven miles. The longer axis extends north and south. The Homer field, as developed in 1902, included parts of Burlington, Bennington, Washington and McKean townsbh‘ps, Licking county; and Milford, Miller and Morgan townships, Knox county. Lying between these two reservoirs were those at Thurston and Newark, but as already stated both have been abandoned. By reference to the map accompanying this article it will be seen that the several tracts named form parts of a belt extend- ing north and south. The length of this is about sixty miles. History and Development. No other event ‘in the history of Ohio has so stimulated the search for underground wealth as did the discovery of natural * Published by permission of Edward Orton, Jr., State Geologist. HARRISON UNION Tre AMERICAN GEOLOGIST, VOL. XXXI. Le Mt. Vernon LIBERTY HARRISON ess [Wea = al ae el dic rd WALNUT MADISON H oO PERRY THORNTON & RIGHLAND ae Prats XIV. CENTRAL CHIc NATURAL GAS F po ome jo be Es et i SS ors. Vaile) Ss) Ohio Natural Gas Fields.— RBownocker. 219 gas at Findlay in 1884. From that as a center drilling has radiated in all directions until every county in the state has been tested; in some the wells may be counted by scores, in others by hundreds, and in a few by thousands. From the areal standpoint these tests have in the main produced neg- ative results only, and yet they form the basis of one of the state’s principal sources of wealth. The Findlay discovery was followed a year later by that of oil in the Trenton lime- stone, and in 1887 by natural gas at Lancaster. The first step towards testing the rocks in the vicinity of the town just named was taken in December, 1885, when the .Lancaster Natural Gas Company was organized. In the fol- lowing May the first well was begun, the objective stratum being the Trenton limestone. On February rst of the ensuing year (1887) gas was found at a depth of 1957 feet; and though the well was small, the mere presence of the desired fuel was sufficient to secure further tests. Two additional wells were drilled that year in the same general vicinity, and with similar results. Preparations were at once’made to pipe the town; and the new fuel finding immediate favor, the com- pany was not able to meet the demands, owing principally to the expense of laying the necessary mains. All the wells drilled thus far were small, so that the out- look for the territory was not bright. In fact during the winter of 1888-9 the supply had so far decreased that it did not meet the moderate demands then existing. The situation changed suddenly, however, in February, 1889, when a new well, “The Mithoft” was completed. This had an open flow of 12,000,000 cubic feet per day, changing at once the character of the ter- ritory. Another famous well was completed that year. It was located on the county fair grounds and had an initial open flow of 10,000,000 cubic feet per day. A line from this well was laid around the race track that fall and “By this means the track was lighted up at night as never was race track lighted before, and the trials of speed went forward under this wanton illumination. The idea was novel and the scene unique and brilliant, but the waste was barbaric all the same.”* In the spring of 1888 the city, by authority of the Legisla- ture, bought the existing natural gas plant, extended the mains, * Geol. Sur. of Ohio, First Ann. Rep. (1890), p. 237. 220 The American Geologist. ADEA nena. drilled new wells, and in other ways prepared to profit by the discovery which the enterprise of a few citizens had made pos- sible. The next thing was to find a market for the new fuel, and “‘the strange folly that seems bound up in a municipal cor- poration when it obtains a good supply of gas, that it must find some one who can use the fuel up in the largest way and most rapidly to whom to give it, without money and without price broke out also in Lancaster. An ill-omened arch bearing the illumined inscription ‘Kree gas to manufacturers’ spans the main street of the town at the railroad crossing.’’* The efforts of the city to secure factories through the offer of free gas were not successful as they had been in northwestern Ohio, and consequently Lancaster did not experience the boom that Findlay and adjacent places enjoyed. ‘The results, however, were good, the city being better in every material way than before the discovery. Newark was another of the towns stimulated by the work at Findlay. The first well, drilled probably in 1885, did not reach the Lancaster gas rock, but in October of the following year another well was begun which after considerable delay reached the gas rock, the depth being 2385 feet. A small flow only of gas was found, but it was sufficient to secure further exploration. Accordingly the third well was soon completed but with similar results. Other wells followed in quick suc- cession, and by 1889 the supply was regarded sufficient to warrant piping the town. The wells, however, were small, the best producing only about 1,000,000 cubic feet per day, and in the winter of 1889-90 the supply was not adequate to meet the demands.+ An effort was made to meet the difficu'ty by drilling new wells, but this was only partially successful. The Newark reservoir cannot be regarded as having contrib- uted notably to the fuel supply of the state. In the spring of 1888 a well was drilled at the village of Thurston, which lies between Lancaster and Newark, the re- sult being a small producer of gas. The second well located one mile farther east, had an initial production of 7,000,000 cubic feet in twenty-four hours and a rock pressure of 700 pounds to the-square inch. This started the excitement, and * Thid, p. 236. + Vol. vi, pp. 370-1; also First Ann. Rep. (1890), pp. 237-240. Ohio Natural Gas Fields— Bownocker. 221 by the summer of 1889 sufficient gas had been secured to war- rant laying a line to Columbus. Rapid progress was made so that in January, 1890, that city was enjoying natural gas for the first time. The supply decreased so rapidly, however, that by the ensuing November the company was compelled to dis- continue furnishing the fuel to factories, and by January 15th, 1891, to cut off the city entirely. After that date very little gas was taken from the Thurston field. The number of wells drilled in the vicinity of that village numbered nearly thirty. The short life of this reservoir resulted from the small area and the heavy demands made on it. The quantity of gas con- tained in any rock is limited, and the duration of the supply is determined by the demand; double the latter and the life of the field is cut in two. The length of the territory was three and one-half miles, and the width one-half mile. In February, 1891, a well was completed on the Zink farm, about two miles north of Lancaster, and a production of 6,- 000,000 cubic feet of gas per day secured. Naturally other wells were soon begun, and nearly all were successes. In May, 1891, the volume secured was such that Columbus was again supplied, and since that date the city has enjoyed an uninter- rupted supply of the finest fuel in the world. The next step in the development of the Central Ohio fields was taken September 3, 1893, when a well was completed on the Meesbarger farm about three miles northeast of Sugar Grove. This was a large producer, and the energy of the dril- ler was at once turned to that territory. Work has been con- tinuous from that date, with the result that the producing ter- ritory has been extended into four townships in Fairfield county and three in Hocking. At first the fuel was supplied to nearby towns, such as Logan and Lancaster, but as the ter- ritory was developed and its wealth disclosed, other corpor- ations entered the field and the fuel was piped to more distant places. In this way the demands have become enormous. Five large companies and three smaller ones are shipping the fuel as fast as it can be secured. The territory supplied is well illustrated by naming the cities and the towns that are the principal consumers: in northern and northwestern Ohio there is Toledo, Bowling Green, Fostoria, Fremont, Clyde, Bellevue, Norwalk, Chicago Junction, Caréy, Upper Sandusky, Tiffin, 222 The American Geologist. sia ewes ps Bucyrus, Marion, Mt. Gilead, Mansfield, Galion, Crestline, Shelby, and Ashland; in the central part of the state, Columbus, Delaware, Westerville, Newark, Mt. Vernon, Zanesville, Lan- caster, and Circleville; in the southern and southeastern parts, Logan, Nelsonville, Athens, and Chillicothe; in western Ohio, Dayton, Springfield, Urbana, Piqua, Troy, and Sidney. The original rock pressure of this field was about goo pounds to the square inch, but under the heavy calls made the pressure has become much less. This however varies from place to place; in the fall of 1902 it had decreased to 100 pounds around Sugar Grove, but at other points it was larger, rising occasionally to 600 pounds. This low pressure was not sufficient to drive the gas through the lines to distant points, and in 1900 the companies began the construction of powerful compressors. Later midway stations were built, so at the pres- ent time the rock pressure is strongly re-enforced, and in this manner the lines are kept filled. Probably the largest well in this territory had an initial open flow at the rate of 12,000,000 cubic feet per day; but at the present time wells of one-third that size are looked upon with much satisfaction. Persons familiar with the field estimated that the average quantity of gas per well put into the lines in 1902 was about 250,000 cubic feet per day. It is safe to say that during the year just mentioned at least 60,000,000 cubic feet of gas have been tal:en on the average from the Sugar Grove field every twenty-four hours. This territory has already passed the zenith, and unless extensions are found its production will decrease rapidly. One more paragraph and the historical side of this question will be brought to a close. In July, 1900, a well was completed near the village of Homer in the northern part of Licking county, and began producing about 1,500,000 cubic feet of gas per day. Other wells were drilled within the following year, and with similar results. Late in the autumn of rgor and erly in 1902 larger producers were secured, and consequently dur- ing the latter year work was very active. Nearly all the wells were successes, and ranged in size from about 1,000,000 to 4,000,000 cubic feet per day, the rock pressure varying ordin- arily from 700 to 800 pounds per square inch. The greater number of these were in Burlington township, Licking county. Early in the fall of 1902 a well was completed on the Ohio Natural Gas Fields— Bownocker. 223 Hunter farm in section six of Miller township, Knox county. This had an initial open flow of between 11,000,000 and 12,000,- 000 cubic feet per day. In December following a well was completed on the Miller farm located on the northern part of the same section, the result being a 9,000,000 cubic foot well. Early in January, 1903, a well was completed on the Bein- hower farm in the southwest corner of the same section, and a 11,000,000 cubic foot producer secured. Just north of these giants a number of producers, ranging from 4,000,000 to 6,000,000 cubic feet have been completed. These wells rad- ically change the character of the field. While the territory has not yet been tested sufficiently to demonstrate its lasting quality, the indications are that it will equal the best yet found in the Clinton sand. Several of the largest companies operating in the Sugar Grove field have en- tered this territory, the result being that a number of the prin- cipal cities in the central part of the state are using fuel from the Homer field. This much can be said for the territory at present,—the acreage is large, rock pressure high, gas rock continuous, and salt-water absent below the Berea grit. It will supplement the supply of fuel received from Sugar Grove, and may do much more. Geology of the Fields. As has already been stated the geological relations in the several reservoirs are in the main similar, and consequently may be considered together. Where differences occur specific mention will be made. The gas rock was first classified by Dr. Orton with the Clinton, but later he appears to have been in doubt concerning the accuracy of this determination. From numerous well records, and from samples of drillings collected and examined by the writer, it appears that the gas rock lies near the base of the Clinton formation, being separated from the underlying Medina by a few feet of dark slate. This will be made clear in the following pages :— Well Records. The succession of strata below drainage is shown by the following record of Federal well No. 1, located four miles below Lancaster in the old canal bed. 224 The American Geologist. ADT ae Thickness ot Depth to bottom formation. of formation. Drive pipe (ten inch) 54 feet 54 Jee Shales Oke” 145 White sand, with water Ou 165 ” Sandy shale he erg 200mg Gray shale Gor 200) Sunbury (Berea) shale SON, AAD te Berea grit (cased with 81% inch pipe) 25 ” AGT Bedford shale (red) TORis we Osa ‘ black shale BEG) is, TiO ora ‘Ohio shales. . | white shale T4Q.’ E272 Corniferous, Lower Helderberg and Niagara limestone, 697 ae 1959 ” Top at 1272 ws Sali-water at 1407 Salt-water at 1682 Base of limestone 1959 1944 feet of 654 inch casing ~ White slate. GONns AlOPAS, Red rock Tara 2042 an Limestone shell ee Z2OStes Clinton shales Blue slate, break Aten 2055 ite and sandstone | Shales and limestones 15 ” 2070 Blue slate Re 2O7 5 ain ; Clinton sand top at 2075 feet. _ Bottom of well at 2088 feet. Following is the record of the lower part of a well on the Bauer farm, two miles west of Sugar Grove. Samples of drillings below the Niagara were collected by the writer: Corniferous, Lower Helderberg and Niagara limestones, top at 1430 HEE bottom at 2132 { Shales, light chocolate col- | ored. Little lime 36 | Shales, green and chocolate Clinton shales j colored, the latter fossil- | | | ” and sandstone iferous. Some lime Bi ts Shales, green and chocolate l colored. Much lime he ee | Gas sand at 22A7 wes The following skeleton record of the McNichols well, twen- ty-five miles south of Sugar Grove in Jackson township, Vin- ton county is of interest because it shows the thickness of both © the Clinton and the Medina: Ohio Natural Gas Fields—— Bownocker. 225 Berea grit, top at 888 feet. bottom at G42 °” 720 feet of 8% inch casing. 042 feet of 6% inch casing. Corniferous Lower Helderberg and Niagara limestones, top at 173 Siew bottom at 2200 ME Clinton, top at 2390 bottom at BAGO ee Medina, hard above, but very soft below, top at 2460 ” 2554 feet of 5 °/1¢ inch casing. bottom 2560 Cincinnati series, top at 2560 bottom of well 2860 In the Sugar Grove territory the great lirnestones (Corn- iferous, Lower Helderberg and Niagara) are charged with salt-water, which sometimes completely fills the well. The formation is unbroken, except in the lower fifty feet, where it becomes shaly, so that the transition to the Clinton is not abrupt, and yet it is easily recognized by the driller. Lastly, there is given a skeleton record of a well on the Dunlap farm near Homer in Burlington township, Licking county. Drive pipe (8 inch) , 307 feet. Berea grit, bottom at f eisetine 566 feet of 65% inch casing. Corniferous, Lower Helderberg and Niagara limestones, top at Zw bottom 2074 Pink limestone and shales, top at ZO Aen bottom 2187 Clinton sand, top at FIRS ia te bottom PALO 2” Bottom of well at B22 pars The most interesting feature of this part of the field in comparison with that around Sugar Grove is the absence of water below the Berea grit. As shown in the record just given only one string of casing is used, and that extends merely to the base of the Berea. This greatly diminishes the cost of the wells, and also the chances of water forcing its way down into the gas sand. The Clinton formation.—This outcrops in the southwestern corner of the state. Its area there is very small, forming a mere band around the Cincinnati series, but owing to a tendency to form an escarpment with the underlying formation 220 The American Geologist. ses egy tt NE the Clinton is quite conspicuous. The formation in that part of the state is essentially a crystalline limestone. This is usu- ally delicately colored and is often highly fossiliferous. At places it is a building stone of high grade, but uneven bedding has been an obstacle to its use for this purpose. In one or two counties it 1s burned for lime, furnishing a product of excellent quality. The rock is calcareous in composition, becoming in some places the purest rock of this type in Ohio. The fol- lowing is an analysis of the limestone near Osborn, Green county :* Carbonate of lime 07.14 per cent Carbonate of magnesia ADs ee ses Alumina and oxide of iron 41 Silicious matter .70 99.46 Occasionally in the part of the state under consideration, a thin bed of clay, called by Foerste the Beavertown marl forms the top of the Clinton, and at other points a lean deposit of Clinton ore occupies the same relative position. The earl- iest geological reports of the state spoke of the rock carrying the odor of petroleum, and about forty years ago wells w-th this substance in view were drilled in it. The result, however, was total failure. + Under cover in the northwestern part of the state the com- position of the rock changes, resembling very closely that of the overlying Niagara. This is well shown in the following analysis of the Clinton from near Bowling Green:= Carbonate of lime 49.19 per cent. Carbonate of magnesia AON inane Insoluble residue 7 Hak Veeck abe At Fremont, Sandusky county, the formation has been the source of a small reservoir of gas;$ and occasionally it has yielded a small quantity of oil or gas in adjacent counties. In central Ohio the formation presents a complete change. The limestone has disappeared, and there are found in its place shales of various colors and compositions, and usually an inter- calated bed of sandstone. The shales contain a noticeable * Geol. Sur. of Ohio, vol. vi, p. 728. + Second An. Rep. Geol. Sur. of Ohio (1838), p. 225; also vol. iii, (1878), p. 407. + Geol. of Ohio, vol. vi, p. 728. § [bid., pp. 183-9. « Ohio Natural Gas Fields —— Bownocker. EP quantity of carbonate of lime, this being most abundant in the thirty-five feet above the gas rock. Well drillings strongly in- dicate that the green and chocolate colored shales are inter- stratified with calcareous ones. i The gas rock is a light colored sandstone of moderate grain. It drills hard, suggesting that the parts are well cemented. ~The thickness of the stratum is not definitely known; espec- ially is this true in the Sugar Grove field, where it has rarely been drilled through. The maximum reported from that ter- ritory is thirty-four feet, and the average is perhaps one-hali of that. Around Homer the sand is drilled through; five wells selected at random showing thicknesses of 10, 28, 8, 12 and 18 feet, an average of 15 feet. Below the gas sand there is found a thin bed of shales com- monly ranging from ten to thirty-five feet in thickness. This has a dark color and is succeeded below by dark red shales. Since work nearly always stops before the latter are reached, or when they have been penetrated a few feet, thus making certain that the horizon of the gas sand has been passed, data bearing on their thickness are meager. The record of the Mc- Nichols well, previously given, credits 100 feet to the form- ation. The top of this red rock is regarded as the summit of the Medina. Life of Wells—This depends on several factors, suck as nature of gas rock, closed pressure, initial flow, acreage per well, rapidity with which the gas is used, salt water, care taken of.wells, etc. The short life of the Thurston field has already been noted. That of the territory around Newark was longer because the demands made on the wells were not so heavy. The following table was compiled from wells in the Sugar Grove field. It shows the original rock-pressure and open flow, the decrease of these, and to some extent the life of the wells. The data are taken from wells that have been prac- tically in continuous use. Doubtless records could be secured from this teritory that would show a greater period of pro- duction than any wells contained in this table. April, 1903. The American Geologist. 228 ——— ee ——$— ” ” " ” 9% OLS d é 000'8ZT'L O8S |"LO6LE “AON |""T ‘ON sJaldnq ii " “e 61 OSS d é 000‘000'% | Ser |"1O6T ‘4iINf|'L ‘ON uepuesg e 7” 5 oF FG OZI el d 000‘'00S'L Och | 1LO6T ‘41O[ | "TON rausEIS ” ” ” ” =“: OO- 000'TLS'S TAA 000'TS¥'9 008 | "LEST ‘99d |'"T “ON 49138934 ‘i i 5p & +06 SLI d O€&@ | 000'000'S | OTF |'006T ‘42d |"F ‘ON Spieu pg ‘ZO6T “3d-g ‘poad WS) +81 OST 000'08S'S 008 00S‘0L8'8 Oro =| 668t ‘Ainf Ton qnys ‘LO6L ““qaq peuopueqy| +81 0) 0) 0) 000'FL8'8 OOL |"868T “Idag |G “oN Uapoom r . ‘ r é é pele. 0&6 000'696'6 Oso =| 668T “Uuef|"T ‘oN ueWieY ” ” ” ” aly raat 008's9L's c0G 000°S9T'L O6L |"868T ‘Judy "Ton weay oF re 20 ” +oT CCRT Ac altay Acs eo 3" OFS 000'38S2'8 |. 00S | 668T “AON |" Z ‘ON 42/3897 GOGBE “3deg “posd [INS é OLT 00€ FS1'% Oba) | 00S loess) 068-5] 268 * SON tas L ‘ON Z)0'] ‘TO6L ‘g eunf| +81 0 000'9F2L'T OST OOS‘ TST'L OV. | 2GSiIL. “AON es ON Astog ‘SO6L ‘FG é ) 000‘00S'S OLT 000'000'6 OPL | "LEST “290 |" LON t9zE1q ‘TO6L ‘8ST “AON| +4T 0 000‘094'% | O6T OSS OLS? | 006 | LE8T ‘290 |""T ‘ON pesnog ‘668E ‘41nf| +81 0) ) 0) 000'T9T'L GS a ese} Oni [ON Ass9g : “CO6L “TO6L 6 “your ‘pauopurqe way Ay pas 30 shacson TOoES tea kaso | sat +2 god “Said ‘Poa UyM | “Ta Jo eweN 40 HSVHNOAC] AAI ANV ‘MOT NddQ) GNV HXNSSHAYgd AOOY IVILINI AHL INIMOHS ‘(THI AAOUL) AVINS AHL AO STIAM NI HSHH ATAV IL, Ohio Natural Gas Fields — Bownocker, 229 The table shows plainly the short life of wells in the best territory, where care is taken to prolong their lives. Since the rock pressure of the field is now much lower than it was a few years ago, it follows that wells drilled hereafter will be much shorter lived than those sunk formerly. Salt Water—Operators and drillers are almost a unit in reporting the gas sand free from water. However, the great limestones lying above the Clinton rock are charged with brine in the Sugar Grove field, and this is a constant source of dan- ger, for unless the packer fits tightly the water crowds into the sand, causing serious trouble, and sometimes ruins the well. Around Homer, as has already been stated, no water is found below the Berea grit, and consequently the danger is much smaller. Rock Structure.—The strata in the Sugar Grove field have been considered by some on a@ priori grounds to form an anti- cline, and by others a terrace. Neither, however, appears to be correct. On a line running almost due east and west through Sugar Grove, the rock dips to the east nearly 260 feet in less than six miles, an average of forty-five feet per mile, barom- eter measurement. This shows neither an arch nor terrace extending through the territory north and south. Further, at the village Amanda, eleven miles west of Sugar Grove, the Clinton rock lies 600 feet higher than it does at the last named village. This ex- cludes a possible suggestion that the gas belt may lie in the eastern slope of an arch, as several reservoirs of oil and gas are known to do in eastern Ohio. From Lancaster the rock dips southeast more rapidly than the bed of the Hocking river slopes, as is shown by the increas- ing depth of the wells in the valley of this stream. This ex- cludes the idea of an east and west arch or terrace. The large reservoir known as the Sugar Grove, may be re- - garded as consisting of several small but contiguous ones. This is well illustrated by changes in rock pressure. Thus the rock pressure at Lancaster has long been nil, while the wells on the Zink farm, two miles north of that town, which were drilled in 1891, still have a pressure of from 500 to 600 pounds per square inch. Around Sugar Grove the pressure has dropped to 100 pounds, but a few miles away it is several times chat 230 The American Geologist. eer ees figure. Farther south in Hocking county similar conditions are found. It appears that these small reservoirs are separ- ated by strata that are practically impermeable, and conse- quently that one may be drawn on or even exhausted without materially affecting the adjacent reservoir.. This is a marked contrast with the results experienced in the Trenton limestone territory of northwestern Ohio. Composition of the Gas. Below is given an analysis of gas from the Thurston field, the work having been done by professor C. C. Howard of Starling Medical College. Carbon dioxide .25 per cent. Oxygen hitsiqin ee Olefines HBO. ue Carbon monoxide cree: ; Nitrogen CTO he ane : Hydrogen ak ” Paraffines (Marsh gas etc.) OO<4Aat ean For comparison there is given an analysis, made by the same chemist, of natural gas from the Trenton limestone at Findlay.* Marsh gas 92.61 per cent. Olefiant gas S30 ie ow ee Hydrogen DQG Ne Nitrogen Br OMe ae tee Oxygen S34 te wa Carbonic acid VOOR ron ate Carbonic oxide NS Ola meaiate Sulphuretted hydrogen A2Ouk relies Search for the Clinton in Eastern Olio. Many wells have been drilled within the past few years in the eastern part of the state, especially in the counties border- ing on the Ohio river, for an oil or gas rock below the Berea grit. The object has been to find one of the deeper sands known in Pennsylvania and West Virginia, and if not success- ful in this to proceed until the Clinton is reached. These trials have disclosed an interesting fact with reference to the thickness of the Ohio shales, lying between the Berea grit and the Corniferous limestone. Thus at Lancaster these shales have a thickness of 702 feet, near New Lexington, + Vol. wi. p. L3G. Ohio Natural Gas Fields — Bownocker. 231 eighteen miles farther east, 1160 feet, and at McConnellsville, forty miles east of Lancaster, 1712 feet. This is an average increase of twenty-five feet per mile, and if this rate should continue until the Ohio river is reached, it would mean a thick- ness of over 2,500 feet for the formation. This is in harmony with a test made farther north near East Liverpool where these shales were penetrated to a depth of 2,600 feet without reach- ing their base. It is apparent from this fact that it is prac- tically useless to attempt to develop an oil or gas field in the Clinton in eastern Ohio; and further it may now be regarded as having been demonstrated by the drill that when the Berea grit has been passed in this territory all hope of finding an oil or gas rock is gone. SEpRUCEORE OF THE SOUTHERN PORTION OF THE KLAMATH MOUNTAINS, CALIFORNIA. By Oscar H. HERSHEY, Berkeley, California. In the Klamath 1egion, the observation of strikes and dips, unless followed industriously for a long period and over a broad extent of territory, is a waste of time, as it leads to but one conclusion, namely that the entire region has been broken up by small irregular folds and faults which mask the true character of the structure. In certain areas the dips will be prevailingly in one direction, generally easterly, and give the observer the impression that the formation as a whole is in- clined in that direction, whereas the easterly dips are due solely to a vast number of small, easterly tilted fault blocks. The only satisfactory method of obtaining a correct appre- ciation of the structure in a broad sense, which the writer has found available in the Klamath region, is the persistent follow- ing of contacts between different formations. After several years devoted to that kind of work, one acquires the habit of forming mental pictures of the individual forinations as single great masses of unbroken rock, disregarding the innumerable minor dislocations. It is of this major structure that I propose to treat in this paper. The present degree of deformation of the rocks of the Klamath region is the result of movements at different periods 232 The American Geologist. APF sens: of geologic time. At about the opening of the Quaternary era, the territory was warped into a series of broad, compar- atively low arches and domes. *Earlier, but yet at a time post- Cretaceous in age, the same region had been acted on by oro- genic activity, the result being a series of structurally enclosed basins, separated by broad ridges which were high in compar- ison with those formed at the opening of the Quaternary era.t The products of these two periods of orogenic activity were characteristically different from that of an earlier period which appears to have affected the region at about the close of Jur- assic time. The Early Tertiary and Early Quaternary deform- ations were like those which have been shown to have operated on the Southern Appalachian province in post-Cretaceous times, while the first post-Jurassic disturbance of the Klamath region was essentially of what is known as the Appalachian type, be- ing characterized by great folds and faults, with axes extend- ing for hundreds of miles in a certain direction common to the system. ‘The broader structural features of the Klamath re- gion are principally due to this post-Jurassic disturbance and my remarks in the succeeding pages will treat of it chiefly. The pre-Cretaceous stratified formations involved in the Klamath mountains west of the Sacramento river consist of. three series, a highly metamorphic series of schists, supposed to be of pre-Cambrian age, probably Algonkian, possibly Archean; a series of less highly metamorphosed slates, quartz- ites, limestones and cherts, of an age ranging from early in the Devonian to the close of the Carboniferous period; and a Mes- ozoic series also altered by metamorphic action, but less in- tensely than the Paleozoic series.§ The first series consists chiefly of the Abrams mica schist, which is supposed to have an exposed thickness of about 1000 feet; and overlying it, the Salmon hornblende schist, known to be at least 2500 feet thick. Probably the real thickness of these formations is much greater. i *“Neocene Deposits of the Klamath Region, California,’’ Journal of Geology, vol. x, No. 4, May-June, 1902. + ‘The Significance of Certain Cretaceous Outliers in the Klamath Region, California,’’? Am. Jour. of Sci., vol. xiv, July, 1902. t ‘Geomorphology of the Southern Appalachians,’’ National Geographic Magazine, vol. vi, pp. 63-126. §‘*Metamorphic Formations of Northwestern California,’’ AMERICAN GEOLOGIST, vol. xxvii, April, 1901. Klamath Mountains, California.—Hershey. 233 The Paleozoic series is estimated to be not less than 5000 feet thick and seems to represent continuous deposition in a broad sea basin. The Mesozoic series is divided sharply into two formations, of which the lower was composed of volcanic materials such as andesite and rhyolite lavas and tuffs, intrud- ed by dikes of diorite, diabase and rhyolite porphyry, all now altered to rocks abounding in sericite, chlorite and epidote. This complex of volcanic materials, the Clear Creek series, is overlaid unconformably by several thousand feet in thick- ness of alternating black slates and blue quartzites, with con- glomerates locally developed, the whole taken together as the Bragdon formation, which is supposed to be of about the same age as the Mariposa formation in the Sierra Nevada region and hence late Jurassic. The total thickness of the stratified formations so far as known is about 12,000 feet, but probably a more thorough study of the region will show the real thick- ness to be several times as great. East of the Sacramento river, Diller, Smith and others have shown that there is there developed a Mesozoic series of slates, limestone and sandstones of late Triassic and early and middle Jurassic age, which seems to be totally unrepresented west of the Sacramento river, except in a few small remnants near Redding, its place in Trinity county being occupied by an erosion interval. This region east of the Sacramento river and a narrow strip west of that stream have lately been thoroughly investigated by Diller in mapping the Redding Quadrangle of the United States Geologic Atlas, and its geol- ogy is hardly within the province of this paper. The distribution and relations of the stratified formations of the Klamath region ‘south of the Klamath river, are now sufficiently well known to make the following history of their deposition reasonably certain: ‘The original sediments of the Abrams mica schist were laid down on the sea bottom with comparative uniformity of character and thickness over the entire area. Upon them were deposited the supposed volcanic ashes which have been metamorphosed into the Salmon horn- blende schist. Apparently this also extended beyond the ter- ritory now under discussion. Then these two formations were metamorphosed, uplifted and eroded. The denudation in places cut away the hornblende schist and exposed the mica schist. 234 The American Geologist. APH eee A geologic map of the territory at the close of this period of erosion would probably have displayed an irregular assortment of patches of hornblende schist in a ground work of mica schist. The Paleozoic series was deposited in a comparatively deep sea and extended far beyond the Klamath province. Upon its uplift at the close of the Carboniferous period, it was deeply eroded, so that the earliest Mesozoic formation rests indis- criminately upon its earlier and later members. However, there is no réason to believe that it was anywhere completely cut through and the underlying schists laid bare, except possibly in one very limited area near Lowden’s ranch in. Trinity county, and even there the phenomenon of contact between the Meso- zoic rocks and the schists may be the result of faulting. The Clear Creek volcanic series was spread as a sheet of varying thickness (probably between limits of 200 and 2000 feet) over the entire territory south of the Klamath river, ex- cept possibly not in the vicinity of the present Scott and Shasta valleys. It was then exposed to erosion in the country west of the Sacramento river and leveled off, but it seems not to have been cut through at any place except probably along the northwestern border of the province, in the vicinity of the present station of Delta. A study of the Bragdon formation has developed a curious bit of geologic history of northern California. It was un- doubtedly laid down in a sheet gradually thinning to the west- ward over the entire region of the Klamath river and west of the Sacramento river. It extends only a short distance east of the latter river in the vicinity of Delta and Elmore stations and in this region contains considerable beds of comparatively coarse conglomerate, which wedge out westward by becoming thinner and finer in texture. The pebbles are composed chiefly of the cherts of the Paleozoic series. Now, these Paleozoic chert pebbles could not have been derived in any of the territory from the Trinity mountain westward as, everywhere in that region, the Clear Creek vol- canic series intervenes between the two slate series. Near Delta and Elmore, on the Sacramento river, the volcanic series seems to be thin and discontinuous from erosion preceding the Brag- don epoch, a fact indicated not alone by my own observation Klamath Mountains, California.—Hershey. 2 35 but also by evidence recently communicated to me by Mr. Dil- ler and in that region may be found the source of the Paleo- zoic chert in the Bragdon conglomerates. The explanation seems to be that the eastern shore-line of the Bragdon body of water was just a little eastward from the site of the present Sacramento river, while northeastward from it erosion was effective on a land whose surface formations were largely the slates, limestones and cherts of the Paleozoic series. The absence of marine fossils and the presence of some plant remains in the Bragdon formation may indicate that it was not laid down in the open sea, but in an inland body of water, perhaps brackish in character. The fact which I have endeavored to bring out by this brief resume of a portion of the geologic history of the southern por- tion of the Klamath region is that at the close of the Bragdon epoch of deposition and just preceding the orogenic activity whose products I am about to describe, the territory was under- laid by four practically continuous sheets of rock, a foundation of schists, a thick layer of Paleozoic rocks, a thin layer of vol- canic materials and a thicker layer of Mesozoic sediments. It is by following the contacts between these four layers that the structure of the region may be truly and readily deter- mined. Considered first as to its broader features only, the south- ern portion of the Klamath region may be described as consist- ing of a central ridge of schists, bordered on the west by a great, unsymmetrical geosyncline, and on the east by the west- ern limb of another great geosyncline. The first geosyncline is limited on the west by another belt of. schist, chiefly the Abrams mica schist, which forms the South Fork mountain and is prolonged northwestward to and probably across the Klamath river near Wichiper. The sandstones of the Coast Range region adjoin this schist belt on the west. Mr. Diller has informed me that toward the north, approaching the Klam- ath river, long, narrow belts of schist alternate with narrow belts of sandstone, the latter dipping eastward as though going under the schists. This apparent anomaly is evidently due to a series of faults. It is further evident that the Coast Range formations have buried the western portion of the schist belt which latter may extend, immediately under the sandstone, far toward the coast. 236 The American Geologist. April, 1903. The eastern schist belt emerges from beneath the Creta- ceous sandstones and shales in the Sacramento valley west of Ono, with a width of eight miles and gradually increases as it advances northward to a maximum of about twelve miles west of Scott valley. Southward from the Trinity river, the pre-Paleozoic area is occupied chiefly by the Abrams mica schist, the hornblende schist being confined to narrow strips, but northward from the Trinity river, the hornblende schist spreads out and finally nearly excludes the mica schist as in the valley of the South Fork of the Salmon river. Still. farth- er north, in the mountains west of Scott valley, the mica schist has again asserted its supremacy. The structure within the schist belt is somewhat obscure, but it is certain that there is no sharp folding of the schists as in the areas of newer and less rigid formations. At one time I thought I saw évidences of two narrow anticlines in the schist area south of the Trinity river, but now I am less confident of that conclusion. It appears to me rather that the schists have been elevated to unequal hights in irregular areas without the formation of any clearly anticlinal or other symmetrical types of structure. Mapping, considered in relation to the present topography, is developing the situation and shape of some of the structurally depressed and elevated areas of the schists and little more can be said about them at present. The space between the two schist belts has a width south of the Trinity river of about twenty-four miles and northward in approaching the Klamath river increases to about thirty five miles. It is occupied mainly by the Paleozoic series, although somewhat west of the center there is a narrow belt of Mesozoic rocks, consisting of the Clear Creek volcanic series and the Bragdon slate series. The Paleozoic series is difficult of sep- aration into its constituent members because of its comparative uniformity of chara¢ter throughout, but the presence of Upper Carboniferous fossils just east of the Mesozoic belt as found by the writer at Patterson’s on New river in western Trinity county, and by Mr. James Storrs* (an assistant of Mr. Diller) near Harrison gulch in western Shasta county, makes it evi- dent that the Mesozoic series rests upon the upper members of the Paleozoic series. * Bulletin of the U. S. Geol. Survey, No. 196, Series F, Geography, 31, p.64. Klamath Mountains, California.—Hershey. 237 Along the eastern border, near the schist contact, the Pale- ozoic strata resemble the known Devonian on the opposite side of the schist belt as in Shasta county, particularly in their ex- tremely cherty constitution, and while no fossils have been found to fix positively the presence of Devonian rocks in the western belt, it is safe to assert that in traveling from the east- ern schist belt westward, one traverses progressively (except for a minor folding) higher members of the Paleozoic series until the Mesozoic rocks are reached. The argument that I wish to draw from this premise is that practically the entire thickness of the Paleozoic rocks is present under the Mesozoic belt, and that along the axis of this belt, where the Bragdon slate is at least 1000 feet thick, and the Clear Creek volcanic series probably of like thickness, the base of the Paleozoic rocks where they rest on the schists, must be at least 7000 feet beneath the present surface; probably it is much deeper. Where the Trinity river crosses the axis of the trough, near Hawkin’s Bar, the schists must be depressed to not less than 5500 feet below sea-level. There is no reason for believing that the axis‘of the trough rises materially to the northward or southward within the limits of the area under discussion. The schists in the belt on the east rise to an altitude of 8500 feet above sea-level and those on the west reach nearly or quite 6000 feet. It is very likely that were the base of the Paleo- zoic rocks restored to its position over the crests of these two schist ridges, it would be far above any elevation now reached by these schists. Therefore, any calculation of the depth of the trough based upon the present highest poitts of the border- ing schist ridges will be a perfectly safe one and probably fall far short of the reality. Generalizing broadly, I shall say that this western geosyn- cline of the southern Klamath region is a trough from thirty- five miles wide in the south to fifty miles wide in the north, and 11,500 feet deep relative to its. western edge and 14,000 feet deep relative to its eastern cdge. The eastern geosyncline is even broader and perhaps deep- er than that just defined. Only its western half properly be- longs to the Klamath region and extends from the crest of the eastern schist ridge of Trinity county to the Big Bend region of Shasta county. It includes all that portion of the Klamath 238 The American Geologist. saseaAes = mountains lying east of the Sacramento river. As already intimated, the present writer does not desire to go at length into the structure of that territory as it has been thoroughly studied by Diller whose report on it is not yet issued, but cer- tain general facts have long been known to the geologic public and may be detailed as follows: A considerable area lying just east of the schist belt, in eastern Trinity and western Shasta counties, is mainly occupied by the Clear Creek volcanic series and the Bragdon slate series. Small isolated areas‘of Devon- ian strata appear in this territory in a way to indicate that this Mesozoic series 1s immediately underlaid over a considerable extent by Devonian rocks. These Devonian rocks come out in force from under the Mesozoic rocks east of the Sacramento river. The same Devonian belt extends northward and west- ward to Scott valley in Siskiyou county, where it adjoins the schist area. ; As it will not seriously affect the argument, it is proper to disregard the Mesozoic rocks lying on the Devonian strata in eastern Trinity and western Shasta counties and consider the schist belt as bounded, structurally on the east by a Devonian belt. This is followed eastward by a Carboniferous belt, then by Triassic strata (the Pit shales and the Hosselkus limestone), and these by Jurassic strata (the Bend shales and the Morrison sandstone), the latter carrying us quite to the easternmost point of the Klamath mountain system. The eastern limb of this geosyncline is mostly buried under the lavas and tuffs of the Lassen volcanic region, but at the northern end of the Sierra Nevada region we may have a sug- gestion of it in the presence, as mapped by Diller in the Lassen Peak Folio of the U. S. Geologic Atlas, of Silurian strata fol- lowed on the west by Devonian and this latter by a broad belt chiefly Carboniferous. Strata of Carboniferous and Jura-trias ages occurring in positions not conforming to the above ideal westward succession weaken the argument and I give it as little more than a suggestion. The structural features which have been described as char- acterizing the southern portion of the Klamath region are un- doubtedly not confined to that area. Their extension north- ward will be a matter of future observation. Southward these two geosynclines must underlie the Cretaceous rocks of the Klamath Mountains, California—Hershey. 239 Sacramento valley for a long distance, probably several hun- dred miles. Southward from a line drawn through Weaver- ville, the course is southeast, in conformity with the strike of the stratified rocks of the Sierra Nevada region. Probably the western geosyncline is completely buried under the Sacramento valley and the western limb of the other trough is barely rep- resented, if at all, along the extreme western border. of the Sierra Nevada region where Calaveras rocks appear west of Jurassic strata. Northward from a line drawn through Weaverville, the strata strike north and finally bend toward the northeast, and when the geosynclines pass beyond the Klamath region they are striking toward the interior of the continent. Superimposed on the geosynclines are structural features of the second order such as anticlines, synclines, monoclines and faults. These are especially apparent in the western trough where the Paleozoic and Mesozoic strata have been more or less closely and regularly folded in a manner similar to the Appalachian region. The folding of the Paleozoic rocks is somewhat difficult to work out because of the uniformity of the series, but certain belts of limestone, and in southern Trin- ity county, narrow belts of quartzyte, pass up and down the slopes of the mountains and are apparently repeated three or four times within a half dozen miles in a way to indicate a rather close folding of the series. The Mesozoic rocks of Trinity county lent themselves to this folding action much more readily than did the Paleozoic rocks, and in the Clear Creek and Bragdon area south of Hay Fork village, there are at least three synclinal folds occupied by the Bragdon slate, separated by anticlines in the axes of which the Clear Creek volcanic series outcrops, all comprised within a space of two miles. These folds are persistent along the strike for twelve or fifteen miles. In the western Paleozoic area, long narrow belts of the Clear Creek volcanic series occur folded down into the slates. Four miles below Cecilville, in the valley of the South Fork of the Salmon river, there is clear evidence that there has beer a complete overturn of a limited area so that limestone, slate and chert of the Paleozoic series rest upon tuffs of the Clear Creek series. The contact is the original one, showing a non- conformity, but now upside down. 240 The American Geologist. Gata) The structure of the Mesozoic area of eastern Trinity and western Shasta counties has been partially described by me in several former papers* and little new material can be added. The area as mapped has a length from north to south of about forty miles and a maximum width of about thirty miles with a probable average of twenty miles. It occupies a basin-shaped depression in the surface of the Devonian rocks, which latter, however, do not come to the surface along its western and northwestern borders, partly because of faulting and partly because of the intrusion of vast masses of peridotite along that line. The axis of the basin lies considerably northwest of the center, has a course approximately north-northeast to south- southeast and occupies the position nearly of the present sum- mit of the Trinity mountain. In this central and deeper por- tion of the basin, the Bragdon slate outcrops without inter- ruption over extensive areas, but nearly all around the borders, it has been upturned, eroded and the volcanic series laid bare. The northwestern one-third of the basin is characterized by the development of a system of beautiful anticlines. They strike east-west with a tendency to bend northeastward in en- tering Shasta from Trinity county. The Trinity river between Trinity Center and Eastman gulch, a distance of eighteen miles, traverses about ten of these anticlines. The intensity of the folding reaches a maximum a few miles south of Brag- don where the elevation of the axis of the anticline may be 2000 feet above the same strata in the axes of the bordering synclines. The strata are closely appressed, so that at and near the river-level, the contacts are vertical and in places slightly overturned. From’ this point both northward and southward there is noticeable a progressive decrease in the amplitude of the folding vertically, and lengthening of the rolls, until the system dies out in comparatively gentle un- dulations. If we follow the crest of a given anticline, using the con- tact between the volcanic series and the overlying black slates as our datum plane, we will find it rising and falling in a series of gentle undulations. Also, we will find frequent small faults, with throws of 10 to 100 feet, with a consequent tilting of the **“Origin and Age of Certain Gold ‘Pocket’ Deposits In Northern Califor- nia,’’ AMER. GEOL., vol. xxiv, July, 1899. ‘““Metamorphic Formations of Northwestern California,’? AMER. GEOL., vol. xxvii, April, 1901. Klamath Mountains, California.—Hershey. 241 fault blocks between. The combination of all these structural features has given rise to such a complexity of local dips that anyone crossing the country on one of the stage roads is like- ly to arrive at almost any kind of conclusion in regard to the general structure of the area. Subsequent to the completion of the Clear Creek volcanic series and apparently also subsequent to the deposition of the Bragdon slates, much of the Klamath region was invaded by huge batholiths and dikes of peridotyte, since largely altered into serpentine. The largest area of serpentine occurring in the southern portion of the Klamath region occupies the ex- treme northeastern part of Trinity county and adjoining sec- tions of Siskiyou and Shasta counties. It has a length in a di- rection from northeast to southwest of about forty-five miles and a width between five and twenty miles, but within this area there are other intrusives. It has chiefly invaded the Devonian belt east of the central schist ridge, but also extends into the latter and forms the northwest boundary of the Mesozoic belt. Next there were intruded batholiths of gabbro and pyrox- enyte, mainly within the serpentine areas. Another change in the underlying magma resulted in the intrusion of granite batholiths. These rise in the serpentine areas and in the belts of schists, Paleozoic and Mesozoic slates. Their out- crops usually form oval or elliptical areas, square miles in ex- tent, several exceeding a score. The intrusion of such great masses of eruptive material into the sedimentary rocks must have had scme effect on the structure of the latter, but as yet I have failed to observe any strong evidences of an extensive displacement of the strata. The granite masses appear to be in the form of huge columns, rising vertically through the other rocks. In only one instance, namely, that of Mt. Courtney at the head of the South Fork of the Salmon river, do the strata seem to have been distinctly thrust up around a granite batholith. Here the schists have been upturned, so that a narrow belt of Abrams mica schist completely surrounds the granite. In all other cases observed, the granite seems to have simply replaced part of the form- ations intruded. Of course, in the vicinity of the contact there was more or less disturbance of the stratification by the in- truded granite, but no such disturbance of the areal geology 242 The American Geologist. Sag aa by forcing the surrounding strata into new positions as to be accurately and appreciably represented on an ordinary geolog- ical map. The strata which once held the position now occu- pied by the granite are gone. They either sank into the gran- ite mass and were absorbed or they were raised up vertically and removed by erosion. Contact metamorphic zones as markedly distinct from the regional metamorphism of the surrounding country are not numerous in the Klamath region. The only really prominent one which I have observed was called to my attention by Dr. H. W. Fairbanks. The largest granite batholith, extending from near Igo in Shasta county through the Trinity range te near Lewiston in Trinity county, is bounded on the northeast by the Bragdon series of slates, quartzytes and conglomerates. Adjoining the granite, the sedimentary rocks have been con- verted into a mica schist resembling the old schists of the pre- Paleozoic series. ‘The metamorphic action is apparent to the unaided eye for several hundred feet distant from the granite and by means of a small hand microscope is yet clearly dis- tinguishable at the distance of several hundred yards. Now, nothing of the kind occurs around the granite bath- oliths where they were intruded into formations which were already more highly metamorphosed than the Bragdon slates now are. When the granite rises through the hornblende schist, the border is characterized by breccias of angular fragments of schist embedded in the granite. There is not the least evi- dence of fusion along the contact, but every indication of vio- lent fracture of hard rocks. The strata removed were not fused in place and as the physical conditions which forced up these columns of melted rock preclude the probability of the strata having sank deep into the earth, I consider it practically a certainty that they were raised vertically, blown out by vol- canic force and have long since disappeared by erosion. As the peridotyte intrusions were on a grander scale than those of granitic rocks, we will more surely expect in connec- tion with them to find evidence of the lateral compression of the surrounding strata. Perhaps the folding of the Mesozoic rocks in the Trinity Mountain area in a system which is at var- iance with other folds of the region may have been due to compression by the vast mass of melted peridotyte rising on Klamath Mountains, California.—Hershey. 243 the north. However, opposed to this idea are the facts that close to the border of the serpentine area, the folding is slight, and that the apparent large batholith of serpentine is probably a combination of many smaller batholiths so that perhaps only a small part of it may have been in fusion at one time and thus incapable of exerting much more compressive strain on the surrounding rocks than did the granite batholiths. The serpentine areas interrupt the continuity of the belts of stratified rocks, but do not seriously displace them. From the high specific gravity of the peridotyte, it is not likely that the disappearance of the strata replaced was brought about by sinking, and of fusion in place there is no evidence. _ Probably they were lifted to such a hight that erosion has since removed them. In denying, in the preceding paragraph, that there is any evidence in the Klamath region of fusion, by the heat of the intruded magmas, of those portions of the stratified rocks which once occupied the position now held by that portion of the intrusives which is above the stream-level of the region, I do not wish to convey the impression that there is no evidence of fusion and absorption of the same sedimentary series at greater depth, but simply that erosion has not yet penetrated to the zone in which this occurred. The injection into the comparatively pliable sedimentary strata of material yielding such rigid masses of rock as granite, gabbro and peridotyte would be expected to have a marked effect on a subsequent system of folding of the region. No such effect is apparent in the southern portion of the Klamath region, and I conclude that the folding was virtually completed before the intrusion of these batholiths. The granite almost invariably rises as vertical columns. Following the intrusion of the granite there were systems of dikes injected into the rocks. The majority of these dikes approximate very closely to the vertical. It is impossible to say what deformation may have affected the large serpentine areas, but the small serpen- tine dikes which are very plentiful in the Paleozoic area west of the central schist belt, remain vertical. Had all these bath- oliths and dikes been involved in the folding of the sediment- ary rocks, they should be inclined at various angles, not a few being conspicuously near the horizontal. -444 The American Geologist. April, 1903: Nearly all the contacts between important formations in the Klamath region, where observed, are faulted. Most of these faults are of small throw, not exceeding several hundred feet, and are not worth considering. But there are evidences of several faults of great magnitude and probably more will be discovered in the future. In a former paper* I called attention to two in the Upper Coffee creek region which I denominated, respectively, the Lawrence and Keating faults. At that time I was laboring under the delusion that the serpentine involved by these sup- posed faults is an altered sedimentary, probably underlying the entire region except where gabbro rose from under it, and the recognition of the faults was partly based on this suppo- sition. But now that I have become aware of the true charac- ter of the serpentine as an altered intrusive, I see that the orig- inal argument was weak, but I none the less firmly believe in the existence of these faults. They trend north to south, paral- lel with each other and about one-half mile apart. They have been traced for ten miles. In the case of each, the up- throw is on the east and amounts to between 1000 and 2000 feet. Mica and hornblende schists and serpentine are involved, and the latter has been displaced in such a way as to make it certain that the faulting occurred subsequent to the intrusion of peridotyte. Both are thrust faults and might be considered due to the same comprehensive strain as produced the folding of the region were it not for the evidence which places the peridotyte intrusion between the two. The Lawrence fault runs so close to a granite batholith without any displacement as to suggest that it is of later age. At the same time, acid dikes were intruded along the line, of both faults so persistently as to make it evident that the faulting preceded them. The intrusion of these acid dikes followed closely upon the intrus- ion of the granite batholiths. Therefore, if my observations have been accurate, the faulting was due to a comprehensive strain exerted closely succeeding the intrusion of granite bath- oliths and long subsequent to the general folding of the region. In the paper mentioned above, I have also defined the “Trinity Center Fault.” This is undoubtedly a fact as the actual fault plane between the serpentine on the west and the *““Gold Bearing Lodes of the Sierra Costa Mountains in California,” AMER. GEOL., vol. xxv, February, 1900. Klamath Mountains, California—Hershey. 245 Clear Creek volcanic series on the east has been seen, but upon recognition of the serpentine as an altered intrusive, the evi- dence of the importance (because of great throw) of this fault becomes very weak. Where the same fault is due south of the Trinity river, the Bragdon slate is in direct contact with the schists and I am inclined to believe that it is a faulted contact with a considerable but indeterminable throw. I have long suspected that the profoundest fault of the territory may occur along the contact between the eastern schist belt and the Paleozoic belt west of it. This line runs straight for many miles. Usually the contact goes down from the mountain tops to the valley bottoms nearly or quite verti- cally ; indeed, just south of the South Fork of the Salmon river the contact may be inclined toward the schist area. The horn- blende schist and the mica schist as bordering the Paleozoic rocks change places several times. So far the evidence is in favor of faulting. North of the King Solomon mine, in Siskiyou county, the Paleozoic series has, next to the schists. a formation of squeezed and crushed, fine conglomerate which appears to be the “basal conglomerate” of this series. This basal formation could not here be in contact with the schists unless practically an original or unfaulted contact. At the La Grange hydraulic mine near Junction City in Trinity county, the Paleozoic slates pass over on to the hornblende schists and in places rest upon it horizontally and with such an irregular contact as to pre- clude the idea of faulting. The nature of this line separating the schists from the Paleozoic strata is a matter of considerable interest and should receive attention in the near future. Where I examined the contact between the Paleozoic slates and the schists of the western belt, in the valley of the South Fork of Trinity river, near the mouth of Rattlesnake creek, it is apparently not a faulted one. The surface of the schists seems to have been hummocky and the Paleozoic sediments ac- cumulated first in the depressions. The slates dip northeaster- ly at a high angle and the contact is consequently sinuous on a small scale. The joint planes constitute another structural form present to an interesting degree in the Klamath region, but the study of them has not yet progressed to the point of generalization. Berkeley, Cal., Jan. 13, 1903. 246 The American Geologist. April, 1903. SOME RESULTS OF THE LATE MINNESOTA GEOLOGICAL SURVEY.* By N. H. WINCHELL, Minneapolis. This topic has been chosen at the suggestion of the chair- man of the Section (Prof. W. M. Davis), but with reluctance. The results of the survey have been published fully. Owing, however, to the volume of literature devoted to the Minnesota Survey, it is believed that a condensed enumeration of the chief scientific and economical results of that survey may be of use. (1). At the commencement of the survey, the rocks that are now included in the Upper Cambrian were embraced under the two terms “Lower Magnesian limestone” and ‘Potsdam sandstone.” It soon became apparent that the former embraced three parts, which had been unknown to D. D. Owen and his predecessors. Two of these were individually designated Shak- opee limestone, and New Richmond sandstone (a term adopted from the Wisconsin survey) and the term Lower Magnesian (since rejected by the Iowa Survey in favor of a new term Oneota) was restricted to the main body of the limestone ex- posed in the cliffs of the Mississippi between Hastings and Winona. ‘That these two new parts do not belong in the over- lying St. Peter sandstone is evident from the fact that at var- ious places, as at Red Rock and at Shakopee. The Shakopee was included by Owen, who gave the original names, in his term Lower Magnesian limestone, while the Richmond sand- stone, which lies below the Shakopee was never by him referred to as St. Peter sandstone. The term “Potsdam sandstone’ was also entirely changed from its early application in the Mississippi valley. It was found by stratigraphic studies that the Potsdam sandstone of Potsdam, New York, was represented in Minnesota by a more firm, even quartzitic, sandstone whose habit more nearly re- sembles the original Potsdam, and the term was applied to that. With this transfer it became necessary to apply new names to the friable white sandstones of the Mississippi valley. In de- scending order the parts thus named are, Jordan sandstone, St. Lawrence limestone, Dresbach sandrock, and Hinckley sand- rock, with unnamed shales both above and below the Dresbach sandstone. The term St. Croix was given to these sandstones, * Read Dec. 31, 1902, A. A. A. S., Washington, D.C. The Late Minnesota Survey—W inchell. 247 not including the Hinckley sandstone, but extending from the top of the Jordan sandstone to the bottom of the Dresbach sandstone. These friable sandstones with their accompanying shales and limestones, constitute the Upper Cambrian, and lie non-conformably on the Potsdam which was found to be a part of the Keweenawan. (2.) The geology of the Lower Silurian in the northwest has had a diversified history. Gn making a careful and detailed examination, both stratigraphical and paleontological, in which Messrs. Ulrich, Schuchert and Scofield were the chief colabor- ers, it was found that, while the limestones and shales should be, as customarily, included in the Trenton and Hudson River groups, the Galena limestone is the stratigraphic equivalent of the Trenton proper, and that the stratum which had speci- fically been known as Trenton limestone, as that at the falls of St. Anthony, is in a lower position and should be denominated Stones River [or Birdseye] and Black River limestones, the latter overlying. Based on the prevalent characteristic fossils each of these and the Trenton proper, were subdivided into three parts. The Hudson River formation was identified and divided into Utica and Richmond. In the progress of the Lower Silurian investigations a large number of new species were discovered and described. (3.) The extent of the Cretaceous was found to be greater than had been supposed. It was found on the summits of the granite range in northeastern Minnesota, known as the Giant’s range, at points where the Mesabi iron ore is mined. It is known to extend nearly as far east as the falls of St. Anthony, occurs in Goodhue county and it probably once covered the Mississippi valley if not that of lake Superior, lapping over into Wisconsin and Illinois. (4.) The early Minnesota reports are the first which in America recognized the duality of the Ice-age, based on the occurrence of interglacial deposits. The measurement of the time involved in the recession of the falls of St. Anthony was the first demonstration of the recentness of the last ice epoch.* The formation of glacial lakes about the ice border when the slope of the country was toward the ice, the origin of kames (now called eskers), the superglacial position of the drift while being transported, especially in proximity to the ice margin, * Dr. E. Andrews, of Chicago, had, however, reached a similar result based on the dunes and beaches of lake Michigan. 248 The American Geologist. ' April aie now well-known elements in Pleistocene geology, were new conclusions reached by the’ Minnesota Survey. The existence and cause of lake Agassiz was stated in the first annual report. (5.) Owing to the divergence of the strike of the two im- portant iron-bearing formations in northern Minnesota it was observed that there were two iron horizons, thus separating the Mesabi range stratigraphically from the Vermilion. This observation was continued into: Wisconsin and Michigan by a visit to those states, and the same duality was pointed out in the iron regions of those states and was announced for the first time in the Minnesota report for 1888. This grand dis- tinction having been recognized it required only the application of detailed field observation to complete the elucidation of the stratigraphy of the iron ores. ‘The distribution of the iron ores of the lake Superior district has been wrought out on this basis. It has since been discovered that there is still a third iron horizon in northeastern Minnesota, not mentioning the titanic iron ore of the gabbro. It is the Upper Keewatin, the others being in the Lower Keewatin and the Taconic. (6.) It was the Minnesota Survey that separated the Archean into two non-conformable parts, viz. the Upper and Lower Keewatin, with a great basal conglomerate between them. Others had announced a basal conglomerate at the base of the ““Huronian,” but it appears that by Huronian, in this in- stance, was meant the upper iron ore beds, which are not in- cluded in the Archean, but belong to the Taconic (Animikie). Such non-conformity also occurs in Minnesota, and is well known at the base of the Mesabi iron range rocks. (7.) It was the Minnesota Survey that detected the oldest known rock in the lake Superior region, and placed it at the bottom of the Archean. It is the greerstones that were named Kawishiwin, the bottom rocks of the Keewatin, the supposed earliest crust of the globe. (8.) The Minnesota Survey also reached the conclusion that the great quartzyte formation which cuts quite a figure in the geology of Wisconsin and Minnesota is non-conformable upon the Animikie, and is a member of the fragmented beds of the Keweenawan. This has been named Sioux quartzyte, Barraboo quartzyte and New Ulm quartzyte. It is that which contains the red pipestone (catlinyte) in southwestern Min- The Late Minnesota Survey—Wéinchell. 249 nesota. It is the western representative of the Potsdam sand- stone, of Potsdam, N. Y. The light-colored friable sandstones, both in New York and in the Mississippi valley, lie higher, and are allied to the Calciferous, lately called Beekmantown. The eruptive disturbances which immediately followed this sand- stone in the lake Superior region, causing the widespread non- conformity of the lately friable sandstones, were wanting in the Adirondack region. Hence the difficulty of separating this quartzyte from those later sandstones in the northern part of New York state. This quartzyte seems to be the rep- resentative of the Middle Cambrian, as the Beekmantown is of the Upper Cambrian. (9.) The final conclusion of the Minnesota Survey as to the origin of the Mesabi iron ores refers them to a greensand, which has been altered, affording iron ore by concentration of the iron in certain favorable positions. Cotemporary with this alteration was a concentration of silica, and this was in- creased by oceanic precipitation. The original greensand was found to become pebbles, and to increase into angular masses that were neither sand nor pebbles, but rather breccia. These breccia masses have at first an amorphous crystalline texture and grade into a form of the iron-bearing rock which was named taconyte, and the whole was referred to volcanic action, being different forms of suddenly cooled volcanic glass and rhyolyte, broken and distributed by beach action. While this volcanic debris was undergoing this transformation great quan- tities of silica were set free from the glass, but this silica im- mediately saturated the debris producing spotted jasperoid taconyte and sedimentary jaspilyte. (No. 2 helow.) Having reached this result on the Mesabi range it opened the door to the understanding of the iron ores of the Vermilion range, and at once the rhyolitic forms and aJl the igneous as- sociations of those ores with basic igneous rock, were eluci- dated, thus confirming Wadsworth’s idea of the igneous origin of the jaspilytes of the Marquette region—rather the igneous origin of the rock which later was changed into jaspilyte. Here a few words of caution are necessary. There are three rocks which may be called jaspilyte, and have been so called. (1.) The rock above described, the result of silicification of basic rhyolytes and obsidian. ‘ , 250 The American Geologist. April, 1903. (2.) The siliceous rock resembling the last but evidently resulting from oceanic chemical precipitation, forming long parallel bands intersheeted with greenstone debris and with other sediments, and grading into ordinary slate, or graywacke or into a siliceous greenstone. ‘These bands are not wavy nor curled, nor structurally suggestive of lava flows. (3.) * es - ’ ‘ — = ~ : i “ts . - hos ‘ : \ i }, e mv THH AMBRICAN GEOLOGIST, VoL. XX XI. PLATE XVI, d THE LANSING SKULL. (SIDE AND TOP VIEWS.) La =, Las} Poe RICAN GEOLOGIST. Vor. XXXI. MAY, 1903. Ae ING Rt fine Lelst OCENE GEOLOGY. OF THE: CON- CANNON FARM, NEAR LANSING, KANSAS. By N. II. WINCHELL, Minneapolis. PLATES XV—XVIII.* It is well known that in America for the past twenty years, as formerly in Europe, the question of the Pleistocene age of man has divided geologists and anthropologists into two antagonistic groups. The writer has not participated in this dispute, having been occupied with other lines of geological research. It is true that when he found, in 1877, the quartz chips at Little Falls he considered them pre-glacial, i.e. pre- Wisconsin: In the literature of the lengthy discussion which has arisen concerning those chips and other reported discov- eries of glacial and pre-glacial man in America, will be found nothing further from his pen until 1902, when he had occasion to re-examine the Little Falls locality in the light of the re- sults of the Minnesota Survey touching the Pleistocene geol- ogy of the state. In a chapter in “Kakabikansing,” by J. V. Brower, the writer abandons his first announced opinion and refers these chips to that 'period when the ice was still in the central and northern part of Minnesota, while its dissolution maintained a vastly swollen river in the Mississippi valley at Little Falls. For Little Falls therefore these chips are post- Glacial, but for the state and for the general region, they date from glacial time, i.e. the closing stage of the Wisconsin epoch. The writer therefore approached the question of the age of the Lansing skeleton in an undisturbed and judicial frame *Plates XV and XVI are reproduced trom the American Anthropologist, by p ©rmission of the editor of that magazine. phy 204 The American Geologist. May, 1903. of mind. He made a somewhat careful and prolonged study of the environment and of the materials in which the skeleton lay. He has elsewhere given the result of that study.* He was compelled, by the evident force of the circumstances, to assign the skeleton to glacial time, and more definitely to pre- Iowan time. The materials in which the skeleton lay are of the nature of geest. The material overlying the geest is up- land loess, of the mixed nature of much of the upland loess in southwestern Minnesota and in [owa, formed contemporary with the lowan ice-epoch, but showing some of the effects of the prevailing waters of the valley in which it was deposited. It js not the writer’s intention to review the evidence on which that conclusion is based. Since the writer reached that conclusion, however, profes- sor Chamberlin has published in the Journal of Geology,ta re- markable paper on ‘The Geologic relations of the human relies of Lansing, Kansas,” to which the writer will here give special attention. He has no desire nor interest, nor any predetermin- ation to subserve in sustaining the pre-Glacial (pre-Wiscon- sin) or the post-Glacial age of the Lansing skeleton. He wishes simply to contribute somewhat to the correct interpretation of the facts bearing on the age of the Lansing skeleton. In the discussion alluded to, by professor Chamberlin, oc- cupying thirty-four pages of the Journal of Geology, the first ten pages are occupied by an illustrated introduction and an “academic statement” of the operation of scour-and-fill in river bottoms, concluding with the following: If excuse for this academic statement is needed it is found in its special application to the case in hand; for either action of the kind just set forth is to be accepted as an elucidation of the case, as in the preferred interpretation that follows, or it is to be shown incompetent for such elucidation before we permit ourselves to go back of this action to earlier agencies. It is a vital principle of good practice that the agencies and phenomena nearest at hand be first considered, and if the case requires, be eliminated before recourse be had to more remote agencies. This is peculiarly true when, as in this case, the agencies closest at hand have quite certainly swept away the most of a more ancient record in making their own. The ten pages devoted to scour-and-fill, if they have no application to the case in hand, as appears to the writer. can * Presidential address, G. S. A., Washington, 1902. Bulletin, vol. xiv. + October-November, 1902, pp. 745-779. Published about December 18. Lansing Pleistocene Geology.—W inchell. 265 be set aside as mere academician’s play, but with full accept- ance of the principle quoted above; for with the non-applica- bility of that academic discussion there can be no application of the recent agencies—closest at hand in time—to which it refers. Essential Points of Professor Chamberlin’s Discussion, In the course of the discussion of the special case professor Chamberlin makes the following points: 1. ‘The upland surface is mantled with loess and loam, the main portion of which is probably referable to the lowan stage.”’ 2. The tributary valley is well adjusted in its debouchure upon the bottoms of the Missouri valley. 3. The Missouri river rock-bluffs at the point where the _ tributary valley joins the Missouri “have been abruptly trun- cated by the waters of the Missouri,” recently, i.e. since the vvisconsin stage, meaning thereby that the lateral erosive ac tion of the Missouri has not only uncovered the preglacial rock bluff but has eaten further into it. ‘4. “The tributary valley is not occupied by a constant stream, but by periodic run-off.” The channel at present is in a Slightly aggraded and apparently still aggrading stage. 5. Lhe Missouri valley is in a degradational stage, 1. e. the plane of its bottoms is being sunk deeper between the bounding rock bluffs. 6. The depth of the aggradation deposit at the mouth of the tributary “is not known to me, but it is probably not many feet.’’ 7. The lower three or four feet of the materials pierced by the tunnel “is composed mainly of limestone fragments and earthy debris, a part of the latter seeming to come from the Carboniferous beas, a part from the glacial drift or loess, and a part from the river and valley yesh, in short a rather hetero- zeneous mixture.” 8. “About thrée feet above the floor on the western side there is a definite layer of dark highly calcareous clay less than three inches in thickness, but it does not appear on the opposite side.” g. “Even in the inner end of the tunnel the silt [1. e. the upper part of the materials pierced by the tunnel. N. H. W.] 266 The American Geologist. MY oO is notably mottled, in part irregularly and in part in bands more or less horizontal, as though controlled by stratification, though the staining is probably secondary.” 10. In an offset tunnel at right angles to the original tun- nel, running eastward eleven feet from the place of the adult skeleton, the “silty formation has been slightly fissured along a number of lines by tensional action and the little crevices filled with a grayish-wh‘te, soft deposit that effervesced very promptly with acid, implying calcium carbonate. Here “the vague structure lines dipped eastward irregularly.” 11. The definite clayey band found near the base in the tunnel pinches out toward the west in a few feet, and does not appear on the east side. It is “very homogeneous and pe- culiar, as well as very tresh and calcareous.” 12. Small fragments of “softened limestone” were so abundant in some parts of the walls of the open trench cut by Mr. Fowke that the walls presented a “mottling with white chalky spots made by the spade in mashing and spreading them.” 13. In the walls cut by the spade the main material is a silt “somewhat closely resembling loess,’ but containing frag- ments of limestone, and shale ‘‘and other debris incompatible with a typical loess deposit,” without distinct stratification or assortment, but sometimes presenting “a gravelly aspect.” 14. A few drift pebbles and not a few pieces of charcoal were found in the section, also many land shells and additional bones were found by Mr. Fowke, but no unios. 15. The unio found by Prof. Williston in the roof of the tunnel, though having its valves still united, was perhaps intro- duced through human agency, and is not a reliable evidence of a subaqueous origin of the deposit. 16. The deposit containing the skeleton is of limited ex- tent, formed by wash, “‘but not a stream deposit, nor a lake de- posit nor any other form of purely subaqueous deposition. I should identity it as a typical aggradation deposit of the ravine and basal slope type when the hillside environment was Car- boniferous limestone and shale mantled with loess.” This idea is illustrated by fig. 13. (Fig. 1. of this paper.) 17. “The material of the one distinctly water-laid layer was probably derived from the Carboniferous shales at some 100 Fee, —— cc qcry» Fig.1. Section across the tunnel, looking north. special stage of erosion and inundation—some unusual storm and flood perhaps—and was deposited without weathering and remained undisturbed except on its borders.”’ 18. “The main excavation of the [tributary N. H. W.] valley probably dates back to the post Kansan erosion interval, and this was perhaps preceded, and perhaps determined, by a preglacial valley.” 19. “The age of the original valley and of the upland mantles does not concern us here unless these lower deposits, well down in the axis of the valley and at its junction with the great river bottoms, are surely inheritances from the older period, and not adjustment phenomena.” 20. The tributary of the Missouri is narrow, steep-sided, ‘steep-bottomed. It may be occupying an antecedent valley above its mouth but the adjustment phenomena at its mouth indicate that it is in a new channel fashioned by recent agen- cies. ; 21. It is a rare case where a new channel exactly coin- cides with the old channel, as when for instance in the creation of the Missouri river by many antecedent tivers—the later channels would rarely be in coincidence with the earlier [say pre-lowan]| channels, especially at their debouchures upon the valley of the Missouri. 22. The Wisconsin glacio-fluvial deposits are wanting at Concannon’s; and, assuming that they have been carried away by the Missouri, there is less reason to expect that the lighter and more erosible fluvio-glacial deposits of the Iowan are preserved. 23. The human relics are in “a little relic-bearing deposit,” formed by a combination of agencies. The Missouri river flowed past the site with a surface about level with the floor of the tunnel. In floodstage it rose twenty feet higher and built a floodplain as high as the “little relic-bearing deposit” 208 The American Geologist. May, 1903. ascends, i. e. about twenty feet above the upper surface of the limestone forming the floor of the tunnel. The Missouri was diverted to the other side of its channel. There was a wash from the adjacent hills, the little tributary contributed its own flood wash, the limestone and the shale were mingled with the debris, a little drift (Kansas age) came from the region, and the human remains were buried either in the latest part of the erosive stage or earlier part of the flood-plain-building stage. This all took place since Wisconsin glaciation. “The antiquity of the burial is measured by the time occupied by the Missouri river in lowering its bottoms, two miles more or less in width, somewhere from fifteen to twenty-five feet, a very respectable antiquity, but much short of the close of the glacial invasion.” Professor Chamberlin’s points separately considered. y It may be conducive to the proper appreciation of these con- clusions to consider them, by number, somewhat seriatim, and to make sundry references and comparisons. No. I, we have no reason to call in question. We will simply remark that it necessitates the extension of the same Iowan loess into all pre-existing valleys and gorges except where it can be shown that it has been replaced by some later deposit, or has been excavated without replacement. The pre- sumption is that it subsists in the old valleys. It is therefore the first general fact that confronts the unbiased investigator. The writer would refer here to the discussion of the upland Iowan loess and its methods of accumulation and its composi- tion and variation by Mr. W. J. McGee in the eleventh annual Report of the United States Geological Survey,* and to the— epitome recently presented in the writer’s retiring address to the Geological Society of America. If one be seeking for agencies “closest at hand in time” he may ignore this great fact, but in so doing he might ignore the agencies closest at hand and most obtrusive in nature. No. 2. There is no reason to question the present approxi- mate adjustment of the flood-plain debris of the tributary with the flood-plain debris of the Missouri. It could hardly be otherwise with any stream that has a little flood-plain of its own at the point of debouchure upon a larger stream, what- * Op. cit., Pleistocene History of Northeastern Iowa. Lansing Pleistocene Geology.—Winchell. 269 ever may have been the earlier history of their relations. Such present adjustment, however, has no necessary causal relation to the past history and relations of the two streams. It is but the expression of the present moment, and, in this case, bears no significant relation, in the opinion of the writer, either to the past history of the streams or to the question under investi- gation. These streams, as it appears to the writer, have had a long history, with mutual adjustment relations, going back to a remote point in Pleistocene time. 3. The statement made in No. 3 may be true, but it has no bearing on the question in hand. It is, however, open to grave doubts, since it requires work of the Missouri river since Wis- consin glaciation which is in excess of what is known of river action on stratified limestones within the area of Wisconsin glaciation. This need not be discussed because of its non-im- portance, as will appear. GEOLOGY a fA OF THE CONCANNON FARM Tha Regeants covered byihe lowan Loess s With Hansan Drift on Ihe Uplands me “ ° c it 7+ ee t te strikeot he { a coe We | =p ( ee BOE Soe ‘ - opie nue pe 1s ; lance of tbe: hesee Tine vibatary Creek 4 Ex . i ’ PS aie oaks me an Ree kel) OME fee ty Bene Sera , , : ® bs q ie} age = we? Shae aa ig Oe ei 2 Concannd = gare eis Shal LENE ig de Othe >. SH Ke 2}. SESS » Farm House \ eR ~ BAER ae Ei eb Sy ¥ AY sere ce | Ber oe % ‘ mM > le = s ~~ ota Pe eH ‘ Rese Pep Ameston® bare &: sped ae . be =. i : « > = x SCAISE br x. One Halt Inch =100 Feet Shes Fig. 2. Map orapart of the Concannon Farm, 270 The American Geologist. Mary, nae 4. At this point it will be necessary to refer to the follow- ing diagram; in which A represents the point at which the lowest rock appears in the creek bottom. At this place there is a little rapid spot and a good watering-place for horses. The rock exposed is the same stratum as forms the floor of the tunnel. B represents the most eastern point at which rock mm situ is seen in the south bank of the tributary creek. C and D are points situated in the creek valley directly eastward from A and B, but on a line coincident with the average line of the Missouri bluffs as they strike past the mouth of the tributary. E is the entrance to the Concannon tunnel. F is the entrance to the open tunnel. G is the quarry on the north side of the creek. H is the place of the skeleton. The plan is approxi- mately drawn to scale. As to the temporary nature of the creek, it is found, by following it up, that the valley extends about a mile westward, formed by three tributaries that drain about one square mile, and that it is wide and deep, but rarely showing rock, compar- able with its appearance at its mouth. Mr. Michael Concannon has stated in writing: “In my memory, some thirty or more years, the creek has never been dry above A, while below that point it is dry every summer. Between the cellar and A there is no rock vissible, but the ledge that is in the creek bottom at A is the same that is in the floor of the cellar. The distance from A to C is five hundred and ten feet. The distance from B to D. is ninety-six feet. We have never discovered any rock in the north bank of the creek. The quarries on the north side are about seventy-five or eighty feet higher than the cave level, [and] near the top of the river bluff. Immediately east of the [entrance of the] tunnel the creek has excavated its bed twenty feet or more, while a little further east we had a well twenty- four feet deep and did not strike bedrock.” Piles were driven thirty feet in the alluvium in the construction of the railroad bridge over the creek at its mouth. Here is a creek valley, therefore, which has been excavated in the rocky structure of the Missouri river bluffs at least sev- enty-five or eighty feet, from the quarries on the north bluffs down to the level of the floor of the tunnel at E. and thence (say) twelve feet to the level of the creek’s flood-plain, and Lansing Pleistocene Geology.—Winchell. 271 deeper still at least twenty-four feet below the surface of the creek’s flood-plain — in all, a known excavation in the Carbon- iferous limestones and shales a perpendicular gorge one hun- dred and eleven feet deep, with a probability of fifty feet still deeper at the creek’s mouth, and at least fifty feet of strata lying above the quarries on the north side. In other words, this little “periodic run-off” develops, on being examined, into a constant stream occupying an ancient gorge that dates prob- ably from pre-glacial time. Whether the present channel is “aggrading”’ at the present time, while the bottom land of the Missouri adjacent is in a degradational stage (No. 5) is beyond the scope of the writer’s immediate apprehension. He can only state that it would he a condition of contrariety at the point of junction of two streams which appears singular, if not inconceivable, and es- pecially in the light of the perfect adjustment which is affirmed (in No. 2) as a concomitant condition. 5. Whether the bottom land of the Missouri at the Con- cannon farm is at present being lowered as the resultant effect of scour-and-fill, or is being raised, the writer has no positive data by which to form any opinion. That the Missouri river once flowed past the site of the Concannon farm with its sur- face from fifty to seventy-five feet lower than at present, as all along its course in its pre-glacial gorge, there is abundant evidence to show. That this deep rock-cut gorge was affec: by the recurring glacial epochs cannot be questioned, and that it was filled to its brim, and sometimes beyond, by the Iowan epoch is demonstrable. That this filling was by water at cer- tain latitudes, by silty water at others and by silt, called valley loess, at others is perhaps equally demonstrable. That this start- ified valley loess, at still higher latitudes, grades insensibly into the upland loess, losing gradually its preference for the immed- late valley, and pari passu its water-laid structure and assort- ment and that this loess has been re-excavated by the stream, is in the opinion of the writer as evident as any geologic principle of Pleistocene time. That this re-excavation: was interrupted by the waters resulting from the Wisconsin epoch of glacia- tion, and the action was reversed, so that a refilling began, is proved by the Wisconsin terraces that now rise higher than the river level. That the Wisconsin terraces toward the north 272 The American Geologist. May ON are composed of northern gravel derived fram the Wisconsin glaciers, but toward the south are formed of whatever mater- ials the surrounding country could supply, and that they de- scend southward faster than the present descent of the rivers that formed them, so as to disappear by submergence under the wider bottom lands, are propositions that are admitted by most Pleistocene geologists. That the Misscuri has, in some places, excavated a channel into the deposits of the Wiscon- sin epoch, forming Wisconsin terraces, and ai others has filled its pre-Wisconsin channel by additions to its flood plain, is quite certain. That this excavation should be toward the north and this re-filling toward the south is also quite certain. Whether the Concannon farm is above or below the point of transition from the latest re-excavation to the latest refilling, it is impossible, from any data at hand, for the writer to state. It seems to be below, and therefore that the present resultant of scour-and-fill at that point is a small addition to the hight of the flcodplain. But owing to the importance attached to this by the hypothesis urged by professor Chamberlin the reader will find a more ample discussion of it under No. 22. 6. The shallowness of the aggradation deposit at tle mouth of the tributary is very important to the hypothesis of professor Chamberlin. If it is deep enough to show ex- cavation in the rock in the manner of a gorge it implies that the creek occupies an inherited channel, ard that the Mis- souri also must have been running at a lower level when that gorge was excavated, and no such event has taken place since the Wisconsin ice-epoch. The statement of Mr. Michael Con- cannon that a well sunk twenty-four feet in the creek bottoms a little east of the mouth of the tunnel did not encounter bed _ rock and that piling thirty feet long was driven for the support of the bridge, is all the information the writer has bearing on this point directly. But inferentially he has much evidence that the creek had a pre-glacial adjustment with the pre-glacial Missouri at a considerable depth below its present adjustment plain. In the first place, the whole surrounding topographic contour shows that this creek’s valley is exactly like almost innumerable tributary valleys that enter the Missouri and the Mississippi rivers south of the Wisconsin morainal belt. There is no topographic, nor other; reason to exempt it from the - any Lansing Pleistocene Geology—Winchell. 273 uniform character and history of the region, viz: the creek occupies an inherited pre-glacial valley, and its buried adjust- ment with the trunk stream must be many feet below the- present floodplain, the intervening distance being the measure of the thickness of the total aggradation deposit. In the second place the sinking of the water of the creek every sum- mer, as stated by Mr. Concannon, below A in figure 2, and its never disappearing above A, indicates that it does not flow on the rock from A to C, but on the contrary that it enters at A upon a mass of loose aggradation deposit into which it sinks at once. Again, the fact that the massive, level lime- stone layer that constitutes the floor of the tunnel, say twelve feet above the top of the creek’s aggradation deposit, is cut away from C to A, a distance of 510 feet up the creek’s val- ley, shows that there was a water-fall during this period of cutting; for this layer of limestone is underlain, at the en- trance to the tunnel, by more shaly and erosible beds. Tfrom B to A this water-fall (or rapid) must have receded, and at an earlier date also from C to B. Such durable layer of rock, lying between shales above and below, not only must have caused a sudden increase in the descending gradient of the stream, but must have been the primary cause of the excava- tion of a gorge in the softer shales lying below. Hence it is easy to infer, given the creek, and the limestone layer, that there is more or less of a gorge all the way from C to A, now filled by the aggradation deposit in question. It is not neces- sary to dwell on this point. It is impossible to discuss the age of this little creek in an impartial and thorough manner and exclude such early history. 7. The statement made in No. 7 must be explained by reference to some preconceived idea on the part of the author supplemented by a hasty and casual examination on the spot; for the facts, as ascertained by the writer, are quite at variance from it. The thickness of materials to which professor Cham- berlin here refers rarely, if ever, reaches four feet. But, what- ever it may be as to actual thickness, it will be assumed here that he refers to the water-laid silt (3 in. thick) and the ma- terials that underlie it. In this the writer could find no “earthy debris,” properly so called, no “glacial drift,” no “loess” (like that which overlies the silt layer, or that which mantles the 274 The American Geologist. May, 1903. general region), nor any “river valley wash,” nor any “het- erogenous mixture.” It is a homogeneous, uniform, exceed- ingly fine,, non-effervescing clay, containing only debris from the adjacent Carboniferous strata, its nature being more that of a residuary clay than anything else that the writer ever saw. In its lower portion, and at higher levels where the skel- eton was found, are masses of Carboniferous limestone, but the leaching and rotting have been so thorough that the cal- cium carbonate is not appreciably distributed in the matrix in which they lie; but each limestone mass is surrounded with a coating, from half an inch to two inches thick, of its own un- disturbed residuum. Hence they are slippery, when wet, and’ unhandy to move or to break with a hammer. These large limestone masses are more and more frequent toward the face of the tunnel, being almost wanting below the silt layer at the entrance. The writer made a microscopical ex- amination of the substance below the silt layer. After repeat- ed decantation from a handful washed repeatedly in a Jar, from which therefore the finest grains were cupposed to have been removed, he was surprised to find that the finer of the remaining grains and all the coarse ones, were perfectly homo- geneous and uniform grains of itself. These homogeneous grains showed, still, that they were compound, and consisted of aggregations of grains of an excessively fine substance. A number of mountings were made, in an effort to ascertain the nature of the ultimate particles. In each instance the mounted grains showed still their composite structure: until, at last, the very dust ,that adhered to the white paper from which the visible grains had been shaken off, was put’on the slide and covered in Canada balsam. Scattered amongst some still compound grains were seen, in the highest powers, the is- olated, ultimate grains of the substance. They appeared to: be entirely of ragged fragments of kaolin, never showing any roundness that could be attributed to friction under trans- portation. When aggregated these fine particles interfere with the transmission of light, and, owing probably to the presence of a small amount of iron oxide, the small clusters appear nearly opaque except at the extreme ends of small pro- jections: This oxide also gives the brown stain which char- acterizes the clay in bulk. Lansing Pleistocene Geology.—W inchell. 275 A similar examination was made of the stratified silt layer, with similar results. If casually examined this silt would be pronounced highly calcareous—and so it is en gros. But it is apparent, on closer inspection, that this carbonate of lime is largely confined to loess-kindchen formed in it, or to encrusta- tions and fillings that occupy the numerous fissures by which it is cut. These fissures are very numerous and very tortuous. They cause the dry silt, when excavated, to crumble into a thousand polygonal masses that roll out almost spontaneously. They are abundantly coated with a white deposit of carbonate of lime. When thoroughly washed and freed from this second- ary deposition of carbonate of lime, these masses do not effer- vesce freely on the application of hydrochloric acid, but if they be immersed in such acid there appears a languid attack of the acid in the escape of a few fine bubbles of gas, showing that the secondary deposition has also penetrated the inter- ior of the silt. There is another slight difference observable in the microscopical mounting, viz: the silt contains also round- ed or angular grains of quartz of much greater size than any seen in the clay underlying. But with those two exceptions this silt is, microscopically and chemically, identical with the clay that underlies it. The character of those two layers, taken together, seems to indicate a common origin for the bulk of the material of which they are composed; and also that the silt is referable to a washing action from the under- lying clay; such action having also introduced some coarser quartz particles not derivable from the immediately underlying clay though probably from the surface adjacent. The absence of drift materials from the clay and its scantiness in the silt indicate that they originated in pre-lowan time. The addition cf lime in excess to the silt is due to the downward leaching from the overlying loess. The sample of the silt examined by the writer was obtained near the entrance to the tunnel. He is not able to affirm that the little fissures are as frequent, and as calcareous, at the other end of the tunnel, but he noticed no difference. His sample from the underlying clay was obtained near the place of the skeleton. The writer is under obligations to Dr. C. P. Berkey for the determination of the percentages of carbonate of lime in Nos. 1, 3 and 4. He has made the following statement: 276 The American Geologist. eames Prof. N. H. Winchell, Dear Sir:—Analysis of the samples of material for lime content gives the following results: No. 1. (Natural) Lime (CaCO;) =1.co9% No. 1. (Washed) Lime (CaCO;) =0.975% No. 3. (Natural) Lime (CaCO;) =3.550% No. 4. (Natural) Lime (CaCO;) = 5.207% No. 4. (Washed) Lime (CaCO;) = 5.23 % Minerological Laboratory. Charles P. Berkey. These analyses indicate a considerable increase of carbonate of, lime in No. 4 over No. 3 (from the roof of the tunnel), due to downward leaching, whether washed or unwashed. It is quite probable that the feeble apparent attack of acid on No. 4 when washed is in a large measure due to its fineness of grain. Microscopical examination of the loess (No. 3.) overlying the silt layer disclosed grains of several minerals found in the crystalline rocks, such as feldspar, hornblende, magnetite and, most frequent of all, quartz. These are from 10 to 100 times the size of the ultimate grains found in Nos. 1 and 4. 8. The silt layer is very evident on the west side of the tunnel. Its fissured character has been described. After the tunnel had been extended further by Mr. Fowke, and an off- set had been excavated toward the east, the characters at the inner end of the tunnel, in the east side, as described by pro- fessor Chamberlin, seem to show that the stratified silt layer actually does appear on the east side. These characters are mentioned and quoted in his words under No. 10.* g. There is no call for adverse comment on Nos. g and Io, for the writer saw the same features. Those mentioned under No. 9 are particularly interesting as they show the wide ex- tent of the structure lines apparently controlled by stratification in the main loess deposit. They are probably more evident in situations near the Missouri river than in the sheltered angles, and therefore they apparently increase toward the east. Still, in the eastward offset tunnel cut by Mr. Fowke the material is wholly geest, and shows no horizontal structure lines like those seen in the loess of the main tunnel. The * Later examination shows that the eastward offset referred to is excavated entirely in the fine geest, with few residual limestone fragments. The vertical jointage described by Prof. Chamberlin pervades the whole mass of geest, both here and on the face of the tunnel. Lansing Pleistocene, Geology.—W inchell. 277 writer's sample No. 1 was obtained in the floor of the offset tunnel, a little eastward from the place of the skeleton. It. The peculiar character of the water-laid stratum of silt, and its calcareous ingredient have been discussed under’ No. 7. Its marked resemblance to the layer on which it lies, and their remarkable differences, in structure and composition, from the loess that overlies the silt stratum, set them off from the rest of the materials pierced by the tunnel, and require for them an earlier date and a different mode of accumulation. (See Appendix. ) 12. How can a limestone become “softened,” in the or- dinary use of that word, unless it become rotted? Limestone does not soften either by atmospheric exposure or by mois- ture, unless it is chemically so changed that it has lost its car- bonic acid and has acquired water. Such an alteration can hardly be expected in materials deposited by the waters of the: Wisconsin glaciation, much less by operations of flood- drainage within more modern time. These “softened” lime- stone fragments could not have been introduced into this de- posit in their present condition, but they must have rotted m situ. 13. The description of the main material cut by the side tunnel of Mr. Fowke is nearly as the writer would make it— he only would add that the arrangement of the coarse mater- ial, whether of limestone or of “other debris” is sometimes in indistinct horizontal bands or belts, and that the other de- bris is in part of drift pebbles which are also in the main rovtted in situ, indicating a longer age than since Wisconsin time. Rounded quartz pebbles about half an inch in diameter were taken by the writer from some of these belts of coarser debris, all the other pebbles having become so “‘softened” that their positions were shown by white spots, when of limestone, or loose rusty spots when of “other debris.” The “gravelly as- pect,’ moreover, so far as observed by the writer, was con- fined to such horizontal belts, although the rotted stones were seen scattered more or less throughout the mass. The loess- kindchen are notably most abundant in the horizontal gravelly belts. Whether this should be called ‘‘a typical loess deposit” de- pends on what and where the type deposit is found and when 278 The American Geologist. May Pies found whether it were acceptable to all. It is unquestionable that the usual descriptions of loess, published many years ago, and especially those that were applied to the loess, say at Vicksburg, Mississippi, or to most of the southern points along the Mississippi river, would not fit this deposit. There are, however, on record many descriptions, applied to points further north, say in Iowa, in Illinois, in Missouri, South Da- kota and in Minnesota, which will fit this loess deposit. It 1s chiefly due to the research of Mr. W. J. McGee that the ex- treme southern features have been found to fade out toward the north, and to be replaced by what might be styled northern features, and at last by extreme northern features, the loess becoming more and more like the northern drift, and at last even passing horizontally, as well as vertically, into the north- ern (Iowan) till. Some southern geologists long ago con- cluded from studies in southern states that the loess of those states is a deposit contemporary with the northern drift, but they did not elucidate the manner, nor the place, of transition from loess to drift in passing toward thé north. In like man- ner some northern geologists found a contemporary and con- tinuous sheet extending from one deposit to the other and, while announcing distinctly that fact, failed to define fully the manner and cause of such transition. It required examination in a middle latitude (Iowa) where, as already stated, Mr. Me- Gee worked on the Pleistocene history of northeastern lowa with great thoroughness and high appreciation of the problem, to bring this curious fact, so long wholly unknown, to a clear and indisputable explanation and publication. With the light thrown on the nature and origin of the materials of the loess by the descriptions of Mr. McGee, it is obvious that the typical idea of loess is subject to great extension and alteration, and hence that the deposit on the Cancannon farm, overlying the human skeleton cannot at presént be excluded from the cate- gory of typical loess. The writer has fully discussed this at another place,* and will not dwell on it again. He will only add that, in his opinion, there is no feature of the deposit lying over the Lansing skeleton (above the water-laid silt layer) which is incompatible with the designation Joess for the lati- tude and the Pleistocene geology of the region. *Geological Society of America. Presidential addiess, Washington, 1902. Lansing Pleistocene Geology.—Winchell. 279 In order, however, that this transition from the features of the loess to those of the Iowan till may be made to appear widespread, as it is, the writer will add (besides the remarks on the discussion of the South Dakota drift by professor Todd, given under No. 14) the following references: Professor T. C. Chamberlin, indorsed the idea of the trans- ition, horizontal and vertical, of the Iowan till to loess in his introduction to the last edition of Geikie’s “Great Ice Age.” ' Jour. Geol., vol. 3, p. 273, 1895. Professor J. E. Todd, in his description of “the moraines of southeastern South Dakota” (Bull. No. 158, p. 93) men- tions, among the relations of the drift to the loess, a gradual passage from one to the other, essentially similar to that de- EXPLANATION. a Le One HALF-INCH=DFEET so A MOUTH oF THE TUNNEL a B CARBONIFEROUS LIMESTONE = o one Dae G (OWAN LOESS MN ce ae? “oe 7s Ss Soe - o- * . ° Oe - +0 ooeen @ ROTTED PEBBLES = ° ce eau ee e o- ° oooROTTED LINESTONE PEBBLES S =A pen = ae Saye w San T22 ® Fig. 3. Section of the tunnel parallel with the cross-cut of Mr. Fowke. scribed by N. H. Winchell in 1877, in southwestern Minne- sota. There are numerous statements of facts, and some il- lustrations by figures, in the same work, that lead to the same ‘idea. Professor Todd also quotes Chamberlin to the same effect. (Missouri Geol. Survey, vol. 10, p. 210, 1896.) Professor Calvin, in his report on Page county, (Geology of Iowa, vol. XI, p. 446, 1900) clearly describes the pebbly drift-loess of McGee, under the heading ‘flooded valley de- posits.” “In nearly all the valleys of Page county there is. a formation which in some of its phases resembles loess; but in other of its aspects it is clearly an aqueous deposit. It has 280 The American Geologist. ime fairs) evidently been laid down since the valleys reached approxi- mately their present depth, * * * It is yellowish in color, tough, jointed, and obscurely stratified. Unlike loess it con- tains occasional pebbles and pockets of sand. A small green- stone, two inches long and’ showing glacial planing on two sides, was taken from this silt in the bank of North Branch. * 3 3 Above the section described at Braddyville, west of the railway track, there is a body of the clay twenty feet thick and forming a distinct terrace fifty yards or more in wiith at the top. The hard enamelled scales of the garpike, Lepi- dosteus, were found in this bed at Braddyville, the scales re- . taining their proper relations to each other as if the fish had been buried at the time the silt was forming. * * * The same yellow silt is found beneath sandy ‘alluvium in the val- ley of Buchanan creek, east of Braddyville. It is well shown in the bank of the Nishnabotna river west of Essex, where it is overlain by six feet of a fine, loess-like silt and two or three feet of black loam. At the Rankin Brothers’ brick yard at Shenandoah the section of the clay pit shows 3: SME OESS=likes Clays cea Searches eee ee al diesen tte RN Ie OEE 2. Bluish, stratified clay, clearly an aqueous deposit, but flexed more or Jess as if laid down on an uneven St PACE acaeeyo oe ares cui Seven eet ers tea eae OA catty ge Rr 8 ft. Tf. Porous darks eranuilat™ Clay sents s a coke oe te erene an men ste ste ste ste ste ste st ste sik K > 7K > zk > > ‘Nos. 1 and 3 resemble loess, but No. 2 records a distinct episode between the more recent and the more ancient period of loess formation, during which the valley was temporarily flooded.” “The distribution of this deposit is practically universal in all the valleys below a certain level.” Professor Calvin sug- gests two hypotheses for the date and origin of this material— one, that it was deposited during the Kansan epoch by the melting of the Kansan ice, the other that it resulted in the same manner round the margin of the Iowan drift, the latter being the explanation now generally accepted. Page county is one on the southern boundary of Iowa not far from the Mis- souri river, and almost due north from Lansing. Professor J. A. Udden, in describing Pottawattamie cbunty (Geol. Iowa, vol. XI, p. 260) situated a little northwest from Page county, but bordering on the Missouri river, says that Lansing Pleistocene Geology.—Winchell. 281 in the loess, meaning here the upland loess, the lower half of a deposit ninety feet thick, near Loveland, on the Boyer river is “pebbly.” Mr. H. F. Bain gives (Geol. Iowa, vol. 5, p. 276, 1896) important instances of the cotemporaneous deposition of north- ern till in the loess, with illustrations. This is in Woodbury county, bordering on the Missouri, north of Pottawattamie county. He remarks that, for the exposure near Riverside station, the explanation has been offered of a slipping of till and loess from higher levels down into a lower terrace of loess. At another point, however, he claims that, whatever the case at Riverside station, that explanation cannot apply. It is at a_sand pit northeast of the Brugier bridge, and he gives a full page photographic illustration. This exposure is ‘‘about 150 feet above the river, and the till is above any similar deposit known to occur in this vicinity. The exposure shows a bed of typical till consisting of a matrix of dark brown clay, in which are numerous boulders of Sioux quartzyte (one of these is pointed out by the hammer) and other northern rocks, with loess of the usual. character, both above and below. * * * The presence of the till in the loess indicates the cotempor- aneous origin of the two deposits, and it seems clear that in this case the explanation offered for the Riverside exposure cannot suffice, even if in that it be deemed sufficient.” Such descriptions could be multiplied. 14.° These features are usual in the drift-loess further north. They have been mentioned by Todd in his account of the moraines of southeastern South Dakota and their attendant deposits,* although in his descriptions professor Todd strives to sustain a distinction between the loess and all forms of drift. It is plain, however, that such distinction was difficult (see pages 80, 82, 84, 88 and 89, of Bulletin No. 158). The terms till, or pebbly till, pebbly clay, or simply drift, are sometimes applied by him under the force of a theoretical distinction where the term loess would also apply; and in some cases, without a theoretical distinction, would be preferable, especial- ly in those exposures of pebbly “till” which he ascribes to sub- aqueous deposition (pp. 65 and 66). According to Todd char- * Bulletin No. 158, U.S. G. S., 1899. 282 The American Geologist. tie meh coal is a common feature of the loess near its base. Todd also frequently mentions, and sometimes illustrates in his figures, a stratum or several strata, of stratified silt near the bottom of the loess, such as, according to professor Salisbury, are ex- ceedingly rare at the bottom of the loess, and which are com- parable tothe silt layer at the base of the loess at the Concan- non farm. 15. The Unio which was taken from the roof of the tunnel — at the Concannon farm by professor Williston and Mr. Long was shown to the members of the party, and to the writer, at the time of its extraction. It has been stated that its valves were still united, but of that the writer knows nothing fur- ther than the statement of professor Chamberlin, p. 769. In case this Unio were a true fossil, it would be, of itself, suffi- cient proof of the subaqueous deposition of the materials in which it lay. Land shells may form fossils in aqueous depos- its, but never water shells in land deposits. It is, a priori, however, the strongest evidence of sub-aqueous origin of the loess in which it was found, and the agreement which it has with the obvious other features of the deposit serves to ac- cumulate such a weight of testimony in the same direction that it requires the greatest hardihood to attempt to explain it on the hypothesis of land origin of that deposit. 16. The statement here made shows the needlessness of the “academic statement” concerning scour-and-fill, for this complete statement of theory makes no appeal to scour-and-fill. Indeed, it is evident, from the position of the tunnel as shown in fig. 1 (Prof. Chamberlin’s fig. 13), that the Missouri river is shut off from access to the place of the skeleton by the Carboniferous bluff. It might reach it by back-set of water, if it were ever high enough, forming a bayou up the creek’s val- ley, but the operation of scour-and-fiull is confined to the chan- nel of the river. As to the extent of the deposit, containing the skeleton— that is not determined by any facts yet brought to light. It appears to be the same deposit that covers the region. It as- cends the higher slopes, 1.e., unless some distinction can be made to appear by future exploration, fills the ravines and gorges adjacent, and is not terraced or otherwise topograph- ically or areally set off as separate from the loess of the region. Lansing Pleistocene Geology.—Winchell, 283 It would be very useful in this investigation, to make sundry pits or small trenches in the loess round about in order to as- certain the differences, if any there be, between this and the great loess mantle that covers the rocks of the region at this altitude. 17. There is no reason to doubt that the evidently water- laid layer of silt was put there by ‘some unusual flood.” It appears that the Missouri river flowed at that level at that time. Owing to the integrity of the underlying geest it is evi- dent that the river was not at that time in a stage of active erosion. The relations of the silt to the geest imply that the submergence by the river was not changed to emergence be- fore the deposition of the overlying loess. The relations of the silt to the overlying loess imply that, the submergence contin- ued, there was a copious rather sudden deposition of more distantly transported material by the same agent as deposited the silt. The “unusual flood” may have been the rising of the Missouri introductory to the Iowan loessian floods. However broken the record in other places, or however Jimited the pres- ent sheet of silt, where it is intact its record is good and the missing links of the history at other points should be supplied by restoration from the perfect record wherever preserved. 18. The existence of this post-Kansan (or perhaps pre- Glacial) valley should, according to professor Chamberlin, lead any experienced, unbiased, Pleistocene geologist, to expect either a hanging or a buried adjustment of earlier date upon the main stream. As there is no hanging adjustment there must be a buried one as already shown in No. 6, and hence the pres- ent adjustment is “accidental”— one of those inherited acci- dents that post-Wisconsin Pleistocene geology is so filled up with. According to the depth of water stated by Mr. Concan- non, quoted by professor Chamberlin, that early adjustment must be at least ninety feet below the present level of the Mis- souri. It is evident here, and especially by reference to page 752 of the Journal of Geology, that the word adjustment is applied to the hanging or the buried type when brought by professor Chamberlin into contrast with the present adjust- ment, and hence that, if the present has obliterated or aband- oned an old place of adjustment, without having inherited it, 284 The American Geologist. May, 1908. the creek (which must have been the agent in producing the change) must either have cut down a hanging adjustment or must have cut, at its mouth, a new rock-bound channel down to the level of the present adjustment. This achievement is discussed in No. 20. 19. It is quite difficult to see how the age of the original valley, and of the upland mantles can be excluded from any geological investigation of this problem, unless, by an arbitrary and quite precipitate assumption, the deposit in question is entirely a modern accident, and all the surroundings must be made to agree with that accident as a starting-point. But, allowing the exclusion of these questions except. on the speci- fied condition, it appears to the writer that even on that con- dition the age of the original valley and of the upland mantles is very essential to the investigation, for that specified condi- tion as shown in No. 6 is plainly supplied. 20. In other words: it is possible that a tributary creek, rising say 300 feet above the Missouri, running in a valley that is cut in the Carboniferous rocks at least 200 feet, down to the level of the Missouri at Concannon’s and at least 24 feet be- low its present floodplain, may be in its original gorge except near or at its mouth, where it may be in a new channel fash- ioned by recent agencies. If that is possible, it is possible for a creek to get out of its rock-bound gorge at some point above its mouth, and at its mouth to/cut a new gorge at least 100 feet in depth by the »peration of “recent agencies’ —1.e. since Wisconsin glaciation—a task which, so far as known to the writer, no creek has ever accomplished, especially no “‘per- iodic run off.” The valley at its mouth is rock-bound on both sides. If professor Chamberlin’s supposition does not refer to this rock-cut channel, but to the present shifting posi- tion of the little dry channel that meanders through the creek’s — floodplain at its mouth, it 1s necessary to admit that recent agencies have determined its position. But that contravenes his hypothesis, since the creek’s antecedent valley, as already shown once occupied by the creek, continues to the Missouri at the same place underneath the present creek, and the pres- ent floodplain and its little dry channel are but accidents de- pendent on the vicissitudes of every season. If his hypothesis refers to any other stage in the waters of the creek, between its Lansing Pleistocene Geology.—W inchell. 285 present and its pre-Wisconsin condition, or io any supposed earlier floodplain, between its present and its pre-Wisconsin floodplain, the same is true—i.e., all those stages and flood- plains were events witnessed by the antecedent valley in which the creek now lies from its mouth to an indefinite distance toward its source. 21. This remarkable statement, if the writer understands it, is so far at variance with what is known of existing chan- nels, outside the area of Wisconsin glaciatiou, and especially within the loess-covered areas, that, in the opinion of the writer, the truth would be nearer the exact opposite. There is certainly not a stream entering the Mississippr within Minne- sota, from St. Paul to the Iowa state line, that does not flow in a valley that far ante-dates the Wisconsin glaciation, and probably the Iowan, especially at its entrance upon the Mis- Sissippi’s great gorge. If, however, reference is not intended to the general stream valley (which, still seems to be the fact by reason of allusion to the “creation of the Missouri river by the union of many antecedent rivers”) but to the present channels of the streams concerned as they make their shifting ways through the flood- plains, it must be granted that such channels have no stability, and are likely not to be the same for any length of time. They are subject to the floods and droughts of the seasons; and es- pecially is that true if comparison be made between the present floodplain channels and those that preceded the Wisconsin glaciation. But such alternative seems not to have any bearing on the main question, and further, it contravenes the principal hypothesis, which «masks back to the time of the “creation of the Missouri.” (Compare No. 18.) 22. The glacio-fluvial deposits of the Wisconsin epoch may be wanting at the Concannon farm. We have mentioned some considerations (Nos. 5 & 13) leading to the belief that they never existed there in the form of fluvial terraces. If as supposed by professor Chamberlin they have been removed, their existence at some points, in some of the bayous or in some of the mouths of the tributaries, should still be recog- nized. The Wisconsin terraces, if they ever existed along a river like the Missouri, are never obliterated, so far as ob- served by the writer, so as to leave no trace through long dis- 286 The American Geologist. May, 1903. tances. Still, granting that they have been there and have been removed, their removal must have been effected by a river whose water surface was lower than the Wisconsin terrace. The hight of a Wisconsin terrace according to professor F. A, Wilder’s* careful discriminations, in Lyon county, on the Big Sioux river, which is about 300 miles farther up the Missouri val- ley, is ten feet above the adjacent floodplain, continuing to the mouth of the Big Sioux. According to Mr. Upham this ter- race is still visible between the mouth of the Big Sioux and Council Bluffs, the most southern point still being 140 miles from Concannon’s farm. This terrace, so far as known has not been identified at lower points, and it doubtless disappears in the present floodplain of the Missouri river at many miles north of the Concannon farm. Corroborative of this conclusion is the interesting presen- tation of the descent of the Wisconsin terraces by professor J. E. Todd. According to his tabulation the descent of the lower “bouldery terraces” (the Wisconsin terrace?) along the Missouri is as follows (Bulletin No. 158, U. S. Geol. Sur., p. 137), measured by aneroid: Opposite Niobrara its hight is.......... 200 feet. INnObtaral le Si mo Dalkin: Atel ioe rece Senn tee 2G ee Wiarikstorla cep alacasrn tetera aera eee, RAO we Meri ion: eee aK sale ten eee cere ae ee a TOO. Blais Nebrasicassu% o ctae es teem nape toes FLOM Calhoun ta Nebraskay Utaciaoeec te ee eueer LOOALee Bellevue, Neb? (8 ms. Sie. of (Omaha). 70-7 Measured as the crow flies the distance from Niobrara to Bellevue is about 150 miles and the descent is about .93 foot per mile faster than the descent of the river. The distance from Bellevue to Lansing, measured in the same way, is about 150 miles. If the same relative rate of descent were continued below Bellevue the descent of the Wisconsin terrace to Lans- ing would carry it 69.5 feet, below the surface of the river, at Lansing. Owing, however, to the roughness of this calcula- tion, and to the uncertainty of the data on which it is based (aneroid levels), its chief value consists in showing the south- ward lowering of the Wisconsin terraces, and the certainty of their being lost in the present floodplain at an indefinite * Iowa Geological Survey. vol. x, 1900. Lansing Pleistocene Geology.—Winchell. | 287 distance from the latitude of the Wisconsin morainic belt. It is quite possible also that the “lower bouldery terraces” of pro- fessor Todd, rather than being of the age of the Wisconsin ice- epoch are the parallel of the higher gravels in the Big Sioux valley which professor. Wilder ras assigned to the Buchanan gravels, and that the Wisconsin terrace is that of professor Wilder, already mentioned, which lies much lower and must soon disappear in the bottom land of the Missouri. Accord- ing to professor Chamberlin, however, (Jour. Geol. p. 771) the bouldery terraces of Todd “are directly connected with the first and second stages of Wisconsin glaciation.” This goes to show that the Missouri river at Lansing has not had a water surface, since Wisconsin time, lower than the Wisconsin stage at the same place, at least that it has not removed any Wisconsin terrace at that place, and inferentially that no Wisconsin terrace ever existed there.* The view here presented as to the sinking of the Wisconsin terrace below the bottomland before reaching the latitude of the Concannon farm was presented by Mr. Warren Upham in the January, 1903, number of the Grotocrsr. It is his opin- ion that the Wisconsin terrace sinks into the floodplain of the Missouri not far below the mouth of the Platte river. If no Wisconsin terrace ever existed at the place of burial of the human relics, the Iowan loess has there been exposed to surface wash and removal, and no later Pleistocene record has been superimposed so as to erase or obscure the Iowan record. Further, the little tributary creek, dependent at its mouth on the post-Wisconsin elevation of the floodplain of the Missouri, has not only not had any Wisconsin stage of flood- plain higher than its present floodplain, but since Wisconsin time has had no higher floodplain than its present. What and where the Iowan fluvio-glacial deposits may be is quite another question, but, as already stated, the Iowan stage of the Missouri was so high that it not only filled its original gorge but in some places flooded much of the adjacent region. On its retirement its deposits, which we know as loess, strat- ified and semi-stratified, originating in the Iowan till, silted back by the regional subsidence, were cut into by the streams * This regimen of rivers with respect to the Wisconsin terraces bas recently been discussed by Prof. Chamberlin in the Journal of Geology, vol. xi, p. 75, Jan.-Feb., 1903. 288 The American Geologist. May, 1903. which again in the main assumed their pre-lowan valleys. It appears therefore that this process of re-excavation of ‘the up- land valleys has continued to the present without the super- position of any later record, accompanied in the river valleys, as already stated in No. 5, in some latitudes by re-excavafion of the Wisconsin till and terraces, and in more southern latitudes by a gradual increment in the hight of the floodplain of the Missouri. What more natural therefore, or more inevitable, than that along the rivers the lowan loess should be found lodged on all pre-lowan rock-spurs and bluffs, and that all the inequalities of the pre-lowan surfaces should be expressed with greater or less clearness in the contours of the present loessian surfaces. In case, under pre-lowan decay, a firm rock layer, overlain by an easily weathered mass of shale, had form- ed a projecting shelf on which had gathered a mass of geest and semi-geest in pre-lowan time, as appears to have been the fact at the Concannon tunnel, the same sheltering surroundings would also preserve the Iowan loess on that rock-shelf and might produce, as appears to be the fact at the Concannon farm, an imperfect, blind terrace-like platform. Such plat- form, however, would in no sense be an lowan fluvio-glacial terrace, although its materials, in their present pose, might date from Iowan time, and be a part of the Iowan fluvio- glacial deposits. 23. Again, this final summary statement as to the origin of “the little relic-bearing deposit” testifies to the needless- ness of the “academic statement’? as to scour-and-fill, since it makes no appeal to scour-and-fill. The human remains were in, or below, a loess which rises and extends over the surrounding bluffs, formed by the meth- ods of distribution known as Iowan. As shown in No. 22, the Missouri river never flowed, since Wisconsin glaciation, at low stage, any higher than it does at present, and therefore never as- high as the floor of the tunnel, and never formed, since Wiscon- sin time, a floodplain as high as the top of the relic-bearing de- posit. The circumstances of the Auctuation of the Missouri from one side to the other of its channel, of scour-and-fill, of wash from the hill-sides, of changes in the floodplain of the tributary valley, of the demolition of the Carboniferous bluffs and of the Kansan sheet of the drift, are still going on, have Lansing Pleistocene Geology.—Wiinchell. 289 continued since the spreading of the Iowan glaciation; but since Wisconsin glaciation the normal action of the river and of the creek has not risen above its present plane of effective- ness and never higher, even in greatest flood-stage, than the floor of the tunnel. The date of burial, therefore, is to be de- termined approximately by the length of time elapsed since the spreading of the Iowan loess, which, compared with the age of the Kansan drift seen scantily spread on the highlands was an event much nearer the end than the commencement of the Glacial period. What events may have taken place after the spreading of the Iowan loess, during the period of surface degradation an- terior to Wisconsin glaciation, it is not necessary, at the pres- ent time, to enquire, although they may have been competent, perhaps under some such process as urged by professor Cham- berlin, in covering these remains where they were found. That would make their burial pre-Wisconsin and post-[owan. Concise statement of the two views. Professor Chamberlin’s interpretation of the facts requires: 1. A floodplain built by the united action of the creek, the river, and the wash from the adjoining bluffs, in post-Wis- consin time, thirty-two feet more or less above the present floodplain. 2. In order to that, the interpretation assumes that the river flowed, in post-Wisconsin time, at low water stage at 18 feet above the present floodplain, and eroded the shale over- lying the rock constituting the floor of the tunnel. 3. It requires a heterogeneous mixture of floodplain com- position, made by the agents specified, rising from the floor of the tunnel to the top of “the little relic-hearing deposit,” such deposit being different in date, origin and composition from the Iowan loess covering the uplands adjacent, and about twenty feet thick. Those three points comprise the essentials in his theory, all other attendants being of the class of academic statements or intended to establish these three. The writer’s explanation requires: 1. The identity of the bulk of “the little relic-bearing de- posit” with the [owan loess of the region. 290 The American Geologist. semana 2. The recognition of the geest which lies on the rock and rises three or four feet above it, and the Gerivation of the water-laid silt layer by wash from the geest. 3. The impossibility of the Missouri river and the tribu- tary creek being in erosive contact on the floor of the tunnel at low water, since Wisconsin glaciation, or flowing at a higher level than at present, and hence the impossibility of there hav- ing been at the mouth of the creek any Wisconsin terrace, or post-Wisconsin floodplain forty-two feet more or less above the present floodplain. All the rest of the writer’s discussion foregoing is simply attendant on the establishment of these points, necessitated by the glittering phantasma of Pleistocene geology involved in the establishment of the other hypothesis. Some argument has been drawn in favor of the recentness of the burial from the resemblance of the skull to those of the present Indian, and from the freedom of the skull and bones from encrustation. In reply it may be remarked that not onl: is there a tend- ency amongst glacialists to shorten the Iowan ice-epoch, but to unite it rather closely in time with the Wisconsin. The date of the Wisconsin being generally approved, as about 8000 years ago, and the Iowan probably not more than 8000 years older, it appears: that man may have acquired the physical characteristics of the Indian at that comparatively recent date. The burial of the skeleton, as represented by the discover- ers, in the non-calcareous geest, overlain by an impervious silt layer that intercepted the downward passage of calcareous water from the loess above, is perhaps sufficient to account for the non-calcareous condition of the bones. Since the publication of professor Chamberlin’s paper, pro- fessor W. H. Holmes has discussed the same subject in the American, Anthropologist (vol. 4, pp. 743-752, Oct.—Dec., 1902), and has followed the argument and reached the con- clusions announced by professor Chamberlin. He could hard- ly do otherwise. It is a geological rather than an anthropo- logical investigation, as the essential data are involved in geo- logic science. Lansing Pleistocene Geology.—Winchell. 291 APPENDIX A, The following letters throw additional light on the question of the age and nature of the deposit in question. It is evident that the ter- races of the Missouri should have special examination. Note from Professor Williston. Chicago, Feb. 17, 1903. Dear Professor Winchell: Pardon me for not replying immedi- ately to your letter. The clam was dug from the extreme angle of the tunnel, near the door, by Mr. Long and myself, at about seven feet above the floor, that is where the roof joins the wall. We at first thought it was bone, and I did not recognize that it was a cast until after I examined it at Lawrence. The hinge line and markings of both lateral valves were (and are, if they have not since been injured) quite complete. There is no doubt but that it is a river clam, though I did not attempt to identify the species. Why it should have lost its structure and have been replaced by a cast I do not know. The specimen is now at the University of Kansas, with other shells from the walls. Sincerely yours, S. W. WILLISTON. Criticism by Professor Todd. Prof. N. H. Winchell, Dear Sir: I thank you for the courtesy shown me in asking that I should criticise in any way your able paper in reply to professor Chamberlin. I regret that it has come to hand when I have not had time to do the subject justice and yet return it in reasonable time for publication. I can only briefly express some of the opinions I hold on the various questions raised, without presenting very clearly my rea- sons for the same. The frequent gradation of the till into stratified drift and that in turn into loess, both laterally and vertically, I concede cheerfully, but loess, so far as I have observed, very rarely contains pebbles or er- ratic particles larger than half a millimeter in diameter. Particularly is this true remote from glacial moraines. Moreover, mere composi- tion and physical properties, such as unstratified character, presence of concretions and vertical cleavage, do not clearly distinguish it from quite recent flood deposits. The latter are more likely to have er- ratics of some size scattered through them. 1. The point in your paper which strikes me with the strongest novelty, is your conclusion that the terraces of the early Wisconsin stage would pass below the present level of the Missouri above Lans- ing. Since Mr. Upham has arrived at the same conclusion I must believe there must be some reason for the view, though I cannot see it. I know of no other evidence of a crustal change which that would involve, no overlapping deposits, changes of drainage or warping of upland levels. 292 The American Geologist. feat icc Your interpretation of the terraces recorded in my bulletin, No. 158, is not in harmony with my conception of their relations. Perhaps I should say right here that the terrace at Vermilion is not truly a river terrace but a till terrace formed by the ice-sheet in the valley of the pre- glacial stream. It is only lightly veiled with aqueous deposits. With reference to the other examples, inthe first place, we are to expect that all formed in the early Wisconsin stage must fall into one strictly graded series. Some may mark the ordinary stage of a stream when the Al- tamont moraine was forming, these are likely to be stony especially if they are near the level of the bottom of the stream near the moraine. Those noted by Wilder and Upham, if Wisconsin, may be of this kind. Others may mark the flood stage when the ice was receding from the moraine. ‘To this class I would refer the higher terraces of the “Lower Bouldery series,” which are stony in the vicinity of the mor- aine in Dakota, but are composed of fine material further away. These we should expect would be built largely of sediment, more marked in broad reaches of the valley and higher below the entrance of prom- inent tributaries. Since my study of Missouri I have found no difficulty in contin- uing the series through that state to the narrow gorge below Boone- ville where we should scarcely hope to find them preserved if ever formed. It should be remembered also that another moraine as we may call it, though it has several members, was formed somewhat later in the Wisconsin epoch, the Gary moraine. It would be expected that a lower series of terraces might be found less prominent perhaps cor- responding to the recession from that moraine. Such was the conclus- ion reached and published in the Missouri Geological Report, vol. X, pp. 216-17. The correctness of these conclusions may be judged from a consideration of the following terraces arranged in series according to this view, with the hights of each above the ordinary level of the river adjacent. Their locations and relations to the river may be learned from a map and from the U. S. Geol. Survey bulletin, No. 158 and from the Missouri Geol. Report, vol. X. Altamont stage. Gary stage. Niobrara, Neb., 180-210. Yankton, 140. Sioux City, lowa, 125-150. Blair, Neb., go-110. Blair, Neb., 140. Calhoun, Neb., 10o. St. Joseph, Mo., 165-175. Bellevue, Neb., 7o. Kansas City, Mo., 150-160. Wyoming, Neb., about 7o. Sibley, Mo., 100. Lexington, Mo., 7o. Lexington, Mo., r4o. “Tete Saw plains” 70-90. Brunswick, Mo., 150. Jefferson City, Mo., about 100. Glasgow, Mo., 160-175. Booneville, 150-170. These are not all the examples which might be named, and in some cases they are extensively developed. Lansing Pleistocene Geology—W inchell. Ap t298 I visited the Lansing locality last December with some expectation that the remains might prove to have come from the base of the ter- race corresponding to that shown at Kansas City, where some remains of mammals have been found. In such a case it would have been reasonably evident that they dated from early Wisconsin time. In- stead I found them outside of the trough of the Missouri in the base of a deposit forming an ill-defined shoulder in the valley of a small tributary which rises twenty-five to thirty-five feet above the flood plain of the Missouri. It is reasonable to account for the indefiniteness of the shoulder by wash added from the hillside back. The deposit there is of a grayer tint than that upon the hills back, which is rusty and sandy, resembling that on the east side of tne Missouri in this latitude. The bouldery drift is very thin. It is probable that the ice sheet never reached quite so far as this. It seems possible that the pre-glacial valleys were never perfectly filled in the loess stage, whether it was lowan, Illinoisan or late Kansan, and that the water ways were revived along the same lines as before. Then followed a period of rapid erosion of the Missouri valley and a deepening of its tributaries much beyond any former trenching, another filling to the hight of the terrace outlined above, and again excavation of the sediment, which may not however have extended far up the tributaries. We might think the deposit under special consideration to have dated from such a stage, were it not so near the present level of the river. As it is, it seems to me altogether more rational to consider it the extended apex of an alluvial cone, or the “handle,’ so to speak, of an alluvial fan formed by the creek when the Missouri ‘channel was on the east or opposite side of its flood plain. JI could refer to several such deposits in Fremont and Mills counties, lowa, some rising to fully as great a hight above the Missouri. Then the return of the Missouri to the west side would result in the cutting down again of the tributary as it is to- day. Nor would it require more than a few centuries to accomplish such a cycle, under favorable circumstances. 2. ‘The evidence in favor of a deep preglacial valley seems to me hardly complete. The fact that the bottom of the trough of the Mis- souri opposite has been reported ninety feet below the water level does not prove that the river has ever been lower than at present. Scour to that depth has been observed at Nebraska City by Mr. L. E. Cooley, in 1879.* The well twenty-four feet deep reported by Mr. Concannon is the strongest evidence, but is it possible that soft shale underlies the lime- stone there? 3. When I visited the locality there was a narrow tunnel running with the main one, and west of it extending north from the cross tun- nel. As it is not hinted at in Chamberlin’s paper and you say nothing of it I judge that it has been dug more recently, possibly to obtain earth to close the cross tunnel. Its bottom shows an abrupt drop in the surface of the rock floor of about two feet. How would that affect * Report of U.S. Engineers for 1879 80, part 2, pp. 1066, 1071. 294 The American Geologist. May, 1903. the geest hypothesis? Would geest be likely to have so abrupt sur- face under it? I confess that I did not think of geest when I was there. I did not observe much contrast in color or texture from top to bottom except that there were more stony fragments below as one would expect from a waterlaid deposit near a slope of Carboniferous limestone and shale. From our former correspondence and conversation, you will not be surprised at my view. I have not attempted to answer all your strong arguments, but have tried rather to improve the opportunity you have so kindly given me in presenting briefly my humble contribution to the interesting questions involved. Yours very respectfully, Vermilion, S. D., March 7, 1903. J. Ee Ton: Note from Professor Wright. Oberlin, Ohio. Prof. N. H. Winchell, Dear Sir:—I visited the Concannon farm and made my examina- tions soon after you were there the second time, but I did not have opportunity to make the minute observations which you are able to report. So far, however, as I was able to form conclusions, they agree essentially with those presented in your paper on ‘‘The Pleistocene Geology of the Concannon Farm.” I followed down the main tributary valley all the way from its head, to its opening upon the Missouri valley close by the tunnel in question, and followed around the head of the smaller valley which joins the main tributary at right angles to it just west of the Concannon house. From these observations it »seemed perfectly clear that very little rock erosion had been accom- plished by these tributary streams’ subsequent to the deposition of the general covering of upland loess. They have done scarcely more than to remove from the pre-Iowan, (or as I think the pre-Glacial) valleys the loose material which has been carried into them during Glacial times, This is specially clear, as you have pointed out, from the character and extent of the depression immediately in front of the tunnel and ex- tending from the point A in your figure to the edge of the Missouri flood-plain, but which is now filled with loose debris. The stratum of limestone surrounding this depression and forming the floor of the Concannon tunnel is compact and about six feet in thickness. The de- pression has every appearance of being formed by the recession of the waterfall where the limestone was underlaid by shale. From consider- able familiarity with the recession of waterfalls in similar conditions since the Iowan epoch, it is impossible to believe that this small stream would not have required many times the period which has elapsed since then to accomplish its work. I can but regard it, therefore, as pre-lowan, and for the most part pre-Glacial. 5 2. ‘There is no evidence that the water of the Missouri has been higher than it is now since the flooded condition of the Iowan epoch. Lansing Pleistocene Geology.—W inchell. 295 I agree with Mr. Upham in believing that the Wisconsin terraces dis- appear under the present flood-plain long before reaching the latitude of Lansing. 3. The remnant of loess-like sediment in which the tunnel is dug is in a protected place at the point of a ridge forming the bluff of the Missouri valley bounded on the west by the small tributary gorge joining the main tributary at right angles. The situation is one where a portion of the general sedimentary envelope would be protected from the erosion of these small tributaries, but where it would be impos- sible for it to accumulate by creep or wash from higher elevations. The least which can be supposed is that provided for in professor Wil- liston’s explanation, which involves, general. deposition on the margin of the Missouri when it was flowing fifty feet higher than now. But 4. The character of the lower three feet of the sediment in the tunnel in which the skeleton is said to have been enveloped, as you have described it, is such that its accumulation must have preceded the entire period of loess deposition, My only doubt has been as to the exact position of the skeleton with reference to this pre-loessial portion of the deposit. I notice in Mr. Upham’s account that he says “the skeleton was imbedded in the upper foot of a stony and earthy debris that appears to have fallen from a closely adjacent outcrop of Carboniferous limestone which also in a heavy bed forms the floor of the tunnel; or perhaps the bones lay in a slight hollow of the debris.” I should like a little more spe- cific information as to whether the skeleton was really enveloped in the pre-loessial deposit or simply lay in a hollow on top of it. G. FREDERICK WRIGHT. APPENDIX B. It was through the renewed courtesy of Mr. J. V. Brower, president of the Quivira Historical Society, that the writer made recently his third visit to the Concannon farm. He spent two full days at that place, and was accompanied and aided by Mr. Joseph Concannon in making some observations on the walls of the tunnel and on the river bluffs above and below the farm. These observations are more in detail than any that had been made before by the writer, and they serve to elucidate more fully the geology of the place as sketched above. Sub- quently Mr. Michael Concannon furnished the photographic print seen in plate XVIII, made from a negative taken by Mr. M. C. Long, showing the face of the tunnel prior to the work done by Mr. Fowke. At nine places detailed sections each carrying about four feet were made of the west wall of the tunnel (Stations A to 296 The American Geologist. page es 1), with sketches and descriptions, as given below ; excavations were made into the terrace and pseudo-terraces below the house, and into the loess at points south from the house, up the little tributary creek. Several samples were secured for mi- croscopical examination. The walls of the tunnel. The floor of the tunnel dips toward the north or northeast, about one foot in thirty feet. Hence the floor of the entrance is about two feet lower than the floor at the further end of the tunnel. Station A. The first examination was made at the entrance. The different parts of the material penetrated by the tunnel are numbered as heretofore. The diagram seen in Fig. 1, Plate XVII, illustrates the structure at the entrance, drawn to a scale. It has the following description. No. tf is divisible into 1a and 1b, the former at the bottom. No. ta is twelve to fourteen inches thick, composed of angular debris of Car- boniferous limestone and shale, not much rotted, but mingled with finer materials of loess-like color and appearance. No northern drift seen; not geest. The surface of the limerock is a little below the floor. No. 1b, about two feet thick, is more sandy and loam-like, contain- ing loess-kindchen and pieces of limestone. In the upper ten inches, and faintly in the lower portion, are indistinct signs of horizontal as- sortment or structure. Some limestone pieces are four to six inches in diameter. No. 4 is a distinct silt stratum, two and one-half inches in thickness, and runs over the foregoing intact to the very door of the tunnel, with disturbance of continuity only at the very northern end where late weathering may have worn it off. The transition above and below No. 4 is sharp and sudden, as evidenced by the change of color, texture and evident composition. No. 2, extending to the roof, shows here no noteworthy feature, having the aspect of ordinary loess. Its microscopic characters have already been given, Station B. The next examination was made at sixteen feet from the entrance. At this place the tunnel is enlarged two and one-half feet in each direction, causing a rectangular shoulder in the wall. The diagram shown in fig. 2, plate XVII, consists of two parts. That on the right represents the shoulder in the west wall, facing south. The remainder shows the continuation of the west wall of the tunnel. In the south-facing shoulder the layer No. 4 is seen to thin out toa point and disappear in No. 2, at the same time rising slightly toward the west, and not perceptibly toward the south. ee ee ee ee ee ea eS re ee sree oe = i OA Juaunesvyng fO 2) “uy re Ic Pikentene elas = 2 "Limestone . ese 2.39 4.39 1.98 Ala O3::..... » 3.93 BG 2.90 Fe2Qs...... 212 5.50 4.68 e@urs csc: 10.54 14.90 14.15 IWigi @ssees2 Halt ie Wee oen tee eat: OME AT Th ccaceeses Mic OW tee 12219 ablsygaltss 11.34 CaOnee:: Delis LON7T2 Ih I10) Nia Orsay fi wastes eh etree ce, Kia O Ares ean ielen foaces ees flier te) Lee eae Ignition... eplul UES) eas Sogn ae Motalles..s.- 99.50 99.63 98.49 2) | Des eBee alate} aba le 13°—62°-++ Ue a Ears 622 20° PAE aR ae 60° 28’ Spr. Gr.... 3.36 3.316+ I. Pyroxene from basanyte of Kilimanjaro, G. Becker, an- alyst. II. Pyroxene from olivine diabase of Pigeon Point, Minne- sota. A. N. Winchell, analyst. Loc. cit. * AMERICAN GEOLOGIST, vol, xxvi, p. 203. } GusTaAv BECKER. Zur Kenntniss der Sesquoixyd—und titanhaltigen Augite. Inaugural-Dissertation. Universitats Erlangen. 1902. 310 The American Geologist. May, 1903. III. Pyroxene from olivine diabase of Pigeon Point, Minn. Partial Analysis by R. B. Riggs. Bull. 109, U. S. Geol. Survey, p. 36. ; The pyroxene whose composition is given under II above has been called pigeonite by the writer; it is unique in possess- ing an optic axial angle which is quite variable, but always distinctly less than the usual value for pyroxene. That this abnormally small optic angle is not due to the high per cent of titanium dioxide present in pigeonite seems to be quite well established by the work of Becker. In general pyroxenes pos- sess an optic angle which is remarkably constant; angle V very rarely varies* more than two degrees from the normal value which is nearly 60°. In the three known instances* in which the optic angle shows a marked variation from the normal value it has the values: 65° 3’, 66° 44’, and 68°. These are all larger than the normal value, and the variation even here is insignificant when compared with the variation in the pyroxene of Pigeon Point, where the optic angle becomes so small in some cases as to give almost the effect of an uniaxial mineral. Another peculiarity of pigeonite is that in it the optic angle seems to be extremely variable even in a single thin section. These characters of pigeonite can hardly be due to the man- ganese content, since Flink* has shown that schefferite from Sweden with six to eight per cent of MnO has an optic angle of 65%. The only two occurrences of pigeonite at present known are both in Minnesota:—at Pigeon Point, and at Duluth, that is at the two extremities of a single petrographic province. These lines have been written in the hope that they may lead to the discovery of other occurrences of this anomalous pyr- oxene. * Cf. HINTZE. Handb. Mineral, ii, pp. 1025-1029. Range Structure in California.—Campbell. 311 BASIN-RANGE STRUCTURE IN THE DEATH VALLEY REGION OF SOUTHEASTERN CALIFORNIA.* By M. R. CAMPBELL, Washington, D. C. Recently attention has been called to the geologic structure of the mountain ranges of Nevada and southeastern Califor- nia. An attempt has been made to show that they are gen- erally anticlinal in structure, and that the tilted-block type which Gilbert has described, and which is generally known as basin-range structure, is of rare occurrence. The object of the present paper is to show that, although minor folding was observed in the Death Valley region, the mountains are generally composed of huge blocks of strata that have been strongly tilted and then eroded into their pres- ent forms. The region described is traversed by two systems of struc- tures; one extending in a north-south direction, being the southern extension of the true basin ranges of Nevada, and the other crossing these in a northwest-southeast direction parallel with and presumably an off-shoot from the main line of the Sierra Nevada. The movements which produced these struc- tures seem to have been preceded by an epoch of slight fold- ing in which the Paleozoic strata were somewhat deformed. This was followed presumably in Eocene time by faulting and tilting along northwest-southeast axes which formed parallel mountains and valleys trending in the same direction as the Sierra Nevada. In the valleys so formed lakes accumulated, probably through a change in climatic conditions, and sedi- ments having a thickness of several thousand feet were laid down. In these lake beds are the great deposits of salt, gyp- sum, soda, and borax, which have made the region famous. Following this period of sedimentation came one of movement along north-south axes, which lifted and tilted the surface into immense mountain ranges trending parallel with the new axes. Panamint, Death and Amargosa valleys were thus formed, and Funeral and Panamint mountains were raised up between * Abstract of a paper read at the Washington meeting of the Geological Society of America, Dec., 1902. 312 The American Geologist. techy) them. Lakes formed in the new valleys and received sediments similar to those of the preceding period. The age of the second lake-forming period is vaguely re- ferred to late Tertiary. From structural and stratigraphic evi- dence the beds are younger than the lake sediments of Death valley, and they are certainly older than the gravel deposits which mark the Pleistocene period in this region; therefore, they are provisionally classed as Miocene and younger. EDITORIAL COMMENT. HOW LONG. AGO WAS AMERICA PEOPLED? To glacial geology, as much as to archeology and ethnol- ogy, must we look for the answer of this question. On this continent, glacialists find evidences of man’s presence only during the late and closing stages of the Ice age; but the Old World has good proofs that man was there, making and using stone implements, contemporaneous with the oncoming of that age, when an ice-sheet enveloped the northern half of continental Europe and the greater part of the British Isles, reaching south to the upper courses of the Don and Dnieper, to the lower Rhine, and to the Thames. Any estimate of the antiquity of man, therefore, whether in the western or the eastern hemisphere, must depend on the measures or estimates obtained by geologists for the duration of the Postglacial period, and of the much longer Glacial period. For the time since the end of the Ice age, apparently nearly alike in America and Europe, approximate determinations have been given by N. H. Winchell, G. F. Wright, and many other glacialists, as summarized by Hansen, which range from 5,000 to 12,000 years, Their average, or about 8.000 years, may be confidently accepted as near the truth. It is more difficult to secure a probable estimate, on which glacialists will so well agree, for the length of the Glacial per- iod, which is found on both continents to have been very com- plex and long, as measured by years, though short in compar- ison with preceding geologic periods. On both these vast land areas it involved nearly the same sequence in the stages of Editorial Comment. 313 growth and decline of the ice-sheets, in their first accumu- lation, great recessions and readvances, and their final melting away. From the beginning to the end of the glaciation are counted several stages or epochs of growth and wane, the principal times of ice advance and deposition of drift sheets and moraines in North America being named the Albertan, Kansan, Illinoian, Iowan, and Wisconsin stages. Some glacialists have estimated the antiquity of the Kan- san stage of glaciation, when the ice-sheet extended farthest on the west side of the Mississippi, as from fifteen to fifty times as long ago as the end of the Ice age, that is, between 100,000 and 400,000 years ago, while the Albertan stage and the beginning of the ice accumulation were still older. Others, however, recognizing the necessary limitations of the whole time of life on the earth, from the very ancient Algonkian period until now, considered by astronomers and physicists to be perhaps only about 20,000,000 years and quite surely no more than 100,000,000 years, and comparing the somewhat well known ratios of the geologic eras and periods, have con- cluded that the portion of time belonging to the relatively very short Glacial period, in all its stages, cannot exceed 100.000 years. Such a measure of this period would place its Kansan stage some 50,000 to 25,000 years before its end; and the Iowan stage, to which the fossil man of Lansing, Kansas, is referred, would be only 12,000 to _15,000 years ago. These estimates seem to me compatible with the characters of the Kansan and Iowan drift formations. Instead of the great antiquity at- tributed by some to the Kansan drift on account of its plenti- ful pebbles of decayed rock, supposed to have rotted since the Ice age, I would refer these to a much later derivation from stream gravels that had been affected during a long preceding period by subaérial decay, or to glacial erosion from pre- glacially weathered and decaying rock surfaces. The pebbles or eroded rock fragments would hold their form during the glacial erosion, transportation, and deposition, by being then frozen. Again, the patchy occurrence of the oldest till depos- its in some places near the extreme boundary of glaciation, often found on hights but absent from lower ground, I would not refer to subsequent erosion, implying a great lapse of 314 The American Geologist. May, 1903. time, but to originally unequal and patchy deposition, anal- ogous with the tendency of the ice-sheet in its Wisconsin stage to add till to the hights of growing drumlins, in local- ities of their abundant development, while sometimes leaving little till or none on intervening low tracts of the bedrock. With these explanations I think we may accept a moderate estimate of the age of the Kansan drift, consistent with a duration of the entire Glacial period as only about 100,000 years, and with a close relationship of the Iowan and Wiscon- sin stages, both belonging to the Champlain epoch or time of land depression terminating the Ice age. Man lived in the region of the Somme valley, France, be- fore the great elevation of northern lands which caused them to be mantled with snow and ice. From the Old World, the original home of our species, mankind migrated to America at some undetermined time before or during the Ice age. If the migration was contemporaneous with the glaciation of the northern half of our continent, the passage, whether from northeastern Asia or northwestern Europe, or from both, took place along the shores of the sea, where the vast ice-sheet was bordered by a strip of coastal land like that now fringing the Greenland ice-sheet, but which has since been deeply sub- merged. That America was peopled very long ago is ascertained geologically by traces of man contemporaneous with the clos- ing scenes of the Ice age in Delaware, New Jersey, New York, Ohio, Indiana, Kansas, Iowa, Minnesota, and Manitoba. The latest and most noteworthy proof of this was the discovery last year of a human skeleton under loess of the Iowan stage of glaciation near Lansing, Kansas, as described by the pres- ent writer in this magazine last September. At least it is to be said that this is the view very confidently held. by Winchell, myself, and others who have later visited and examined that locality. But a different view is held by Chamberlin, Holmes, and others, who, from their examination of the Lansing section, think the deposit above the skeleton to be more probably refer- able to Postglacial time. With much care and effort they have also worked and written, during the last ten years, against all the geologic evidences, which others have thought acceptable, Editorial Comment. 315 of man in America in the Glacial period. While some parts of the formerly supposed evidences have been shown to be er- roneous, many other observations seem to me to admit only the conclusion that man was here before the end of the Ice age, and, if so, doubtless through a long preceding time. One of the earliest observers in this country to record traces of Glacial man, by flakes from the manufacture of quartz im- plements, was Winchell, in 1877, at Little Falls, Minnesota. Through twenty-five years from that date, being busy with other geologic work in the survey of this state, he was not a participant in the further investigations concerning this sub- ject. Having been silent during the very animated discussions of the past decade, he now comes to the careful consideration of the Lansing discovery which he has presented in foregoing pages, and in his earlier address as president of the Geological Society of America, with no trammels of previous partizan- ship. To my mind, after much study of this new discovery, the evidence of man here in the late Iowan stage of glaciation, as so well reviewed by Winchell, seems entirely conclusive. Ethnology likewise declares, as voiced by Powell in a pro- foundly philosophic paper in The Forum of February, 1898, that man came to America very long ago, and that he has since developed the many and diverse languages, handicrafts, leg- ends and myths, and the physical peculiarities, of the American race. How long ago that migration took place, permitting the racial development of these people, called the American Indians, to begin, we cannot tell definitely, or even approxi- mately, in terms of years. We can only say that before our continental ice-sheet passed its Iowan stage, the American or red race appears, as shown by the Lansing skeleton, to have progressed far in its differentiation from the white, yellow, and black races. : W. U. 316 The American Geologist. May, 1903. REVIEW OF RECENT GEOLOGICAL LITERATURE. Schmalenseeia amphionura en ny trilobit-typ, af Jou. Cur. Mopsere. [Meddelanden fran Lunds Geologisk-Mineralogiska Institution, No. 5. Stockholm, 1903. ] ; Dr. Moberg states that a peculiar and interesting trilobite was found in the collections of the Geological and Mineralogical Institution of the University of Lund labelled as “Limarssonia occulta” [Lin- narssonia was preoccupied by Walcott for a genus of brachiopod], The fossil is stated to have been collected from the zone Agnostus pisi- formis—the lower part of that zone, in close relation to the equivalent of the Andrarum limestone, and so near the top of the Paradoxides beds. The material studied shows the principal parts of the test, the middle piece of the headshield the movable cheek, the pygidium and parts of the body joint, which is carefully described by the author. The dimensions of the parts also are given, and there is a plate of figures showing the aspect of the two shields, etc. Each of the shields is from 1.5 to 1.8 mm. long, and of proportionate width. Dr. Moberg in’ conclusion refers this little trilobite to the neigh- borhood of the Chiruridze, but says that it does not belong to any known family. [It appears to bear the same relation of Chiruride that Conophyrs does to Asaphide or that Achantholenus does to Anomocare; i.e. small, immature form of a large trilobite, or a trilobite arrested in its development in one of its early stages. A larval feature appears.in the narrow annulated glabella, though the closeness of the eye to the gla- bella has an opposite meaning. In any case the trilobite is of interest as carrying down to the base of the Upper Cambrian a type hitherto known only from the summit of the Cambrian, upwards.] «GF. M. The Glacial Geology of New Jersey. By Roittn D. SarisBury ; assist- ed by Henry B. Kimmet, Cuartes E. Peer, Grorce N. Knapp. Vol. V of the Final Report, Geol Survey of New Jersey; Henry B. Kimmet, State Geologist. Pages xxvii, 802; with 66 plates (includ- ing four folded maps in a pocket of the cover), and 102 figures in the text. Trenton, 1902. In New Jersey the central part of the great ice-lobe of New York and New England attained its farthest southward extension, lacking only about 200 miles of the lowest latitude reached by the ice boundary in southern Illinois, at the central and farthest advance of its wider compound lobe in the Mississippi basin. New Jersey is also of great interest to glacialists because there the varied deposits of the glacial drift adjoin the Pleistocene formations of the more southern part of Review of Recent Geological Literature. IF our Atlantic coastal plain, permitting the two series to be compared and correlated as to their age and conditions of origin. Professor Salisbury, coming with a large experience of exploration of the glacial drift in Wisconsin and other states of the upper Missis- sippi region, has worked on the Pleistocene problems of our Atlantic border, in the intervals of other duties, during twelve years. The pres- ent volume is his report on the glaciated northern third of New Jersey. It does not proceed, however, to the desired correlation of the glacial ‘drift with the Lafayette and Columbia formations, well studied by McGee, Darton, and others, on the coastal belt of the southern states. This chief fruitage of the glacial work in New Jcrsey is reserved, to be given, as we may hope, in a later report, which should treat, with ample details, of the Pleistocene series in the southern part of this state. A general description and discussion of the drift and the Glacial period form Part I, in 226 pages. The conditions which lead to the accumulation of glaciers and ice-sheets, the manner in which they affect the surface of a region on which they lie, and the forms and disposition of their deposits, are analyzed in detail, with abundant references to the glacial deposits of New Jersey. The remaining and greater part of the volume deals very fully with local details, describing the terminal moraine, till, striz, kames, eskers, stratified plain and valley drift, loam, brick-clays, etc., mainly arranged under three divisions; the Appalachian region, the Highlands, and the Triassic plain. Referring to the cause of the glacial climate, Salisbury rejects the astronomic theory of Croll, which would give about 80.000 years as the measure of Post-glacial time. Instead, he thinks it to have been a com- paratively short period of 6,000 to 10,000 years, according to estimates by G. K. Gilbert and N. H. Winchell, derived respectively from Ni- agara and the Falls of St. Anthony. The view that the Ice age was due to great elevation of the lands occupied by the glacial drift, as held by Dana, Upham, and Wright, is also rejected; and the submarine continuation of the Hudson river channel, to a depth of 2,800 feet beneath the sea level off the coast of New Jersey, is not mentioned, although it proves so great elevation of this part of our continent about the time of the ice accumulation. Preference is given to the hypothesis of Chamberlin, which attrib- utes glacial conditions to changes in the amount of carbonic acid gas contained in the atmosphere. It is thought that these changes, affecting the entire earth, and tending everywhere to contemporaneous increase or decrease of glaciation, that is, to cycles of glacial and interglacial stages on the borders of ice-sheets, are most harmonious with what is known concerning the North American and European glacial drift and the fluctuations of glaciers in mountain regions. Beyond the prominent terminal moraine in New Jersey, scantier and older glacial drift, referable perhaps to the Kansan stage of the Ice age, is found, in quite irregular and patchy distribution, to a max- 318 The American Geologist. May, 1903. imum distance of about twenty-five miles. Salisbury writes of this. older drift as follows: “The extra-morainic glacial drift is far from constituting a contin- uous sheet within the area where it occurs. A large part of the sur- face has no drift, and where it occurs it is often very meagre, being represented only by scattered bowlders derived from formations farth- er north. Thin beds of drift, two or three feet in depth, are common, while in not a few places/the drift is of considerable thickness, locally as much as thirty feet. “The lack of continuity of drift in this region is in striking contrast with the condition of things north of the moraine, where drift in great- er or less thickness is essentially continuous. It is true that there are frequent outcrops of rock north of the moraine; and it is true that there are, here and there, areas of some size where the drift is thin. But the areas where the drift is very thin are much less extensive north of the moraine than south of it. The relationship may be expressed. in some such terms as the following: North of the moraine, four- fifths of the surface is so deeply covered with drift as to conceal the underlying rock, and the products of its decay; south of the moraine and north of the drift limit, four-fifths of the surface is nearly free from drift. Just as the one-fifth north of the moraine has occasional bowlders and small patches of drift, so the four-fifths of the area south of the moraine, and north of the drift limit, has occasional bowlders, and small amounts of drift in other forms. The amount of drift per square mile on the four-fifths to the south is probably less than the amount on the one-fifth to the north.” Both here and in Kansas the outermost drift appears to the writer of this review to be of less antiquity than is supposed by Salisbury: From the amount of subaerial erosion which he thinks to have been effected by the rains, rills, and large streams, since the deposition of this drift, he concludes that it is far more ancient, as fifteen or twenty times older, than the terminal moraines and their inclosed drift sheet, which belong to the Wisconsin stage of the Glacial period. Although the outer drift is demonstrably the older, its age seems to me to be very likely no greater than four or five times the age of the Wisconsin drift. The decayed condition of the rock fragments in the outer old drift may be due to erosion from surfaces of pre-glacially decayed bedrocks; and the inequalities of distribution of that drift may be of similar charac- ter with the very irregular accumulation of the later drift on areas of drumlins. Originally patchy drift accumulation outside the boundary of the later drift in New Jersey appears more probable than isolation of the drift deposits by subsequent erosion. W. U. Author's Catalogue. 319 MONTHLY AUTHOR’S CATALOGUE OF AMERICAN GEOLOGICAL LITERATURE ARRANGED ALPHABETICALLY, ADAMS, FRANK D. Memoir of Geo. M. Dawson. (Bull. G. S. A., vol. 18, pp. 497-509, portrait, Feb. 1903.) AMI, H. M. Ordovician succession in eastern Ontario. (Bull. G. S. A., vol. 18, p. 517, [abstract.] Feb. 1903.) AMI, H. M. Meso-Carboniferous age of the Union and Riverside formations, Nova Scotia. (Bull. G. S. A., vol. 13,:-pp. 533-535, [abstract.] Feb., 1903.) BASSLER, R. S. The structural features of the Bryozoan genus Homotrypa, with descriptions of species from the Cincinnattian group. (Pro. U. S. Nat. Mus., vol. 26, pp. 565-591, 13038.) BIBBINS, A. (W. B. CLARK anda). Geology of the Potomac group in the Middle Atlantic slope. (Bull. G. S. A., vol. 13, pp. 187-214, July, 1902.) BOWNOCKER, J. A. The central Ohio natural gas fields. (Am. Geol., vol. 31, April, 1903, pp. 218-231.) BROOKS, A. H. Geological reconnaissances in southeastern Alaska. (Bull. G. S. A., vol. 13, pp. 253-266, Aug., 1902.) BUFFET, E. P. Some glacial conditions and recent changes on Long Island. (Jour. Geog., vol. 2, pp. 95-101, Feb., 1903.) CHAMBERLIN, T. C. Has the rate of rotation of the earth changed appreciably during geological history? (Bull. G. S. A., vol. 13, p. 531, [abstract.] Feb., 1903.) CHAMBERLIN, T. C. Distribution of the internal heat of the earth. (Bull. G. S. A., vol. 13, p..530 [abstract], Feb., 1903.) CLARK, W. B. (and A. BIBBINS). Geology of the Potomac group in the Middle Atlantic slope. (Bull. G. S. A., vol. 18, pp. 187-214, July, 1902.) CLARK, W. B. (and G. C. MARTIN). Correlation of the Coal Measures of Maryland. (Bull. G. S. A.,, vol. 18, pp. 215-232, July, 1902.) 320 The American Geologist. Mey CLARKE, J. M. Annotations [to Ruedeman’s discussion of Professor Jaekel’s theses]. (Am. Geol., vol. 31, April, 1908, p. 216.) CLARKE, JOHN M. Origin of the limestone faunas of the Marcellus shale of New York. (Bull. G. S. A., vol. 13, p. 535 [abstract], Feb., 1903.) COHEN, E. i Meteoric iron from N’Goureyma, near Djenne province of Ma- cina, Soudan. (Am. Jour. Sci., vol. 15, April, 1903, pp. 254-258.) COMSTOCK, THEO. B. Memoir of Edward Waller Claypole. (Bull. G. S. A., vol. 13, pp. 486-496, Feb., 1903.) DALY, R. A. Mechanics of igneous intrusion. (Am. Jour. Sci., vol. 15, April, 1903, pp. 269-299.) DARTON, N. H. Juratrias rocks [of the New York City district]. (U. S. G. S., Geol. Atlas, Folio. 83, 1902.) DARTON, N. H. Description of the Oelrichs quadrangle. U.S. G. S., Geol. Atlas, Folio 85, 1902. ‘ DAVIS, W. M. oye The development of river meanders. (Geol. Mag., vol. 10, Decade 4, pp. 145-148, April, 1903.) DAVIS, W. M. a Walls of the Colorado canyon. (Bull. G. S. A., vol. 138, p. 528 [abstract], Feb., 1903.) DODGE, R. E. (and BAILEY WILLIS). General geology of the [New York City] district. (U. S. G. S., Geol. Atlas, Folio 83, 1902.) DODGE, R. E. (BAILEY WILLIS and). Physiographic features of the [New York City] district. (U. S. G. S., Geol. Atlas, Folio 83, 1902.) EASTMAN, C. R. Devonian Fish fauna of Iowa. (Bull. G. S. A., vol. 18, p. 5387 [abstract], Feb., 1903.) EATON, G. F. Collection of Triassic fishes of Yale. (Am. Jour. Sci., vol. 15, pp. 259-269, April, 1903.) ELFTMAN, A. H. Keewatin and Laurentide ice sheets in Minnesota. (Bull. G. S. A., vol. 18, p. 586 [abstract], Feb., 1903.) FAIRCHILD, H. L. . Proceedings of the fourteenth annual meeting, held at Rochester, New York, Dec. 31, 1901, and January 1 and 2, 1902, including pro- Author's Catalogue. 321 ceedings of the third annual meeting of the Cordilleran section, held at San Francisco, December 30 and 31, 1901; with index, con- tents, etcetera of vol. 13; pp. i-xvii, February, 1903. (Bull. G. S. A., vol. 13, pp. 475-583, Feb., 1903.) FOERSTE, A. F. Use of the terms Linden and Clifton limestones, In Tennessee geology. (Bull. G. S. A., vol. 18, p. 581 [abstract], Feb., 1903.) FOERSTE, A. F. Bearing of Clinton and Osgood formations on the age of the Cin- cinnati anticline. (Bull. G. S. A., vol. 18, p. 531 [apstract], Feb., 1903.) CILBERT, G. K. Joint veins: (Bull. G. S. A., vol. 13,. p. 521 [abstracté, Feb., 1908.) GRABAU, A. W. (H. W. SHIMER and). Hamilton group of Thedford, Ontario. (Bull. G. S. A., vol. 13, pp. 149-186, June, 1902.) GRABAU, A. W. Traverse group of Michigan. (Bull. G. S. A., vol. 13, p. 519 [abstract], Feb., 1903.) GRANT, U. S. Geological excursion in the Pittsburg region. (Bull. G. S. A., vol. 14, pp. 3-5, 1902.) GULLIVER, F. P. Cuttyhunk Island [abstract]. (Bull. G. S. A., vol. 13, p. 538. [abstract], Feb., 1903.) HAMILTCN, S. H. Minerals from Santiago Province, Cuba. GProc= seh Acad: Sci., 1902, p. 744: Feb., 1903.) -HATCHER, J. B. The Judith River beds. (Science, vol. 17, March 20, 1903, p. 471.) HEILPRIN, A, The activity of Mont Pelée. (Science, vol. 17, p. 546, April 3, 1903.) HERSHEY, ©: H: Structure of the southern portion of the Klamath mountains in California. (Am. Geol., vol. 31, April, 1903, pp. 231-245.) HITCHCOCK, C. H. Mohokea Caldera on Hawaii. (Bull. G. S. A., vol. U3," De boo [abstract], Feb., 1903.) HOLLICK, ARTHUR. Cretaceous deposits of Staten Island. (U. S. G. S., Geol. Atlas, Folio 838, 1902.) - HOPKINS, T. C. (and M. SMALLWOOD). Some anticlinal folds. (Bull. G. S. A., vol. 13, p. 530 [abstract], February, 1903.) ‘ 322 The American Geologist. May HOPKINS, T. C. Lower Carboniferous areas in Indiana. (Bull. GS. AS), volaeesos p. 519 [abstract], February, 1903.) HOVEY EE. 0: Paleontological collections of the geological department of the American Museum of Natural History. (Bull. G.'S. A., vol. 13, p. 532 [abstract], Feb., 1903.) KEMP, J. F. Memoir of Theo. G. White. (Bull. G. S. A., vol. 13; pp. 516-517, Feb., 1903.) KEYES; G. R. Devonian Interval in Missouri. (Bull. G. S. A., vol. 13, pp. 267- 293, Aug., 1902.) KNIGHT, W. C. Coal fields of southern Uinta county, Wyoming. (Bull. G. S. A., vol. 18, pp. 542-544 [abstract], Feb., 1903.) LANE, A. C. Variation of geothermal gradient in Michigan. (Bull. G. S. A,, vol. 13, p. 528 [abstract], Feb., 1903.) LAWSON, A. C. ; Geological section of the middle Coast ranges of California. (Bull. G. S: A., vol. 13, p. 544 [abstract], Feb., 1903.) DEES WIEEISST: The canyons of northeastern New Mexico. (Jour. Geog., vol. 2, pp. 63-82, Feb., 1903.) MARTIN, G. C. (W. B. CLARK and). Correlation of the Coal Measures of Maryland. (Bull. G. S. A, vol. 13, pp. 215-232, July, 1902.) MERRILL, F. G. FH. Metamorphic crystalline rocks [of the New York City district]. (U. S. G. S., Geol. Atlas, Folio 838, 1902.) } PRESSEY, H. A. Water supply of New York City. (U. S. G. S., Geol. Atlas, Folio 83, 1902.) REID, H. F. Notes on mounts Hood and Adams, and their glaciers. (Bull. G. S. A., vol. 13, p. 536 [abstract], Feb., 1903. RIGGS, E. S. Brachiosaurus altithorax, the largest known dinosaur. (Am. Jour. Sci., vol. 15, April., 1903, pp. 299-306.) RUEDEMANN, R. Professor Jaekel’s theses on the mode of existence of Orthoceras and other cephalopods, with annotations by J. M. Clarke. (Am. Geol., vol. 31, April., 1903, pp. 199-217.) Author's Catalogue. 323 RUSSELL, I. C. Geology of Snake River plains, Idaho. (Bull. G. S. A., vol. 13, p. 527 [abstract], Feb., 1903.) RUSSELL, I. C. The topographic survey of Michigan. (Address, Mich. Acad. Sci., Ann Arbor, March 20, 1903.) SALISBURY, R. D. Pleistocene formations [of the New York City district]. (U. S. G..S., Geol. Atlas, Folio 83, 1903.) SCHRADER, F. C. Geological section of the Rocky mountains in northern Alaska. (Bull, G S. A., vol. 13, pp..233-252,. July, 13902.) SCHUCHERT, CHARLES. On the lower Devonic and Ontaric formations of Maryland. (Proce. U. S. Nat. Mus., vol. 26, pp. 413-424, 1903.) SELLARDS, E. H. New structural characters of Paleozoic cockroaches. (Am. Jour. Sci., April, 1903, pp. 307-315.) SHIMER, H. W. (and A. W. GRABAU). Hamilton group of Thedford, Ontario. (Bull. G. S. A., vol. 13, pp. 149-186, June, 1902.) SMITH, GEO. O. ‘Description of the Ellensburg quadrangle. U.S. §8., Geologic At- las, Folio 86, 1903. STERNBERG, C. H. Elephas Columbi and other mammals in the swamps of Whitman county, Washington. (Science, vol. 17, March 2/, 1902, p. 511.) TURNER, H. W. Post-tertiary elevation of the Sierra Nevada. (Bull. G. S. A., vol. 13, pp. 540-541, Feb., 1903.) UPHAM, WARREN. Geology of Prairie island. (Mem. Expl. Miss. basin, vol. 6, pp. 34-38, 1903.) UPHAM, WARREN. Life and work of Prof. Charles M. Hall. (Am. Geol., vol. 31, pp. 195-198, April, 1903.) VAN HISE, C. R. Presentation of a bust of Prof. T. C. Chamberlin. (Science, vol. 17, p. 475, March 20, 1903.) WARD, H. A. Bath Furnace meteorite. (Am. Jour. Sci., vol. 15, April, 1903, pp. 316-319.) WHEELER, 0; b: Wonderland, 1908. Descriptive of the country contiguous to the Northern Pacific railway,.pp. 107, St. Paul, 1903. WHITE, DAVID. Memoir of Ralph Dupuy Lacoe. (Bull. G. S. A., vol. 13, pp. 509- 515, Feb., 1903.) 324 The American Geologist. May, 1903. WILLIS, BAILEY. Later Paleozoic conditions [of the New York City district]. (U- Ss. G. S:, Geol., Atlas; Folio 83, 1902-) WILLIS, BAILEY (R. E. DODGE and). General geography of the [New York City] district. (U.S. G. S., Geol. Atlas, Folio 88, 1902.) WILLIS, BAILEY (and R. E. DODGE). Physiographic features of the [New York City] district. (U. S. G. S., Geol. Atlas, Folio 83, 1902.) WILLIS, BAILEY. Later Juratrias and early Cretaceous events [of the New York City district]. (U.S. G. S., Geol. Atlas, Folio 83, 1902.) WILLIS, BAILEY. Events of later Cretaceous, Eocene and Neocene times [of the New York City district]. (U. S. G. S., Geol. Atlas, Folio 83, 1902.) WILLISTON, S. W. The fossil man of Lansing, Kansas. (Pop. Sci. Month., vol. 52, March, 1903, pp. 463-473.) ‘WINCHELL, N. H. Regeneration of clastic feldspars. (Bull. G. S. A., vol. 18, pp. 522- 525, Feb., 1903.) WINCHELL, N. H. Some results of the late Minnesota geological survey. (Am. Geol., vol. 31, pp. 246-253, April, 1903.) WINCHELL, N. H. Granite; address at the dedication of the Coronado monument. Mem. Ex. Miss., vol. 7, pp. 87-90, 19038. WRIGHT, G&G. F. Age of lake Baikal. (Bull. G. S. A., vol. 18, p. 580 [abstract], February, 1908.) WRIGHT, G. F. The age of the Lansing skeleton. (Rec. Past., vol. 2, pp. 119-124, April, 1903.) PERSONAL AND SCIENTIFIC NEWS. Mr. Horace V. WINCHELL, of the Anaconda Copper com- pany, Butte, is examining copper deposits in Mexico. Pror, C. R. Van Hise was elected, April 22d, president of the University of Wisconsin. Dr. A. FE. ORTMAN, OF PRINCETON UNIveErsity, has been appointed curator of invertebrate zoology at the Carnegie Mu- seum of Pittsburg. Personal and Scientific News. 325 ArnoLtp Hacue, of the United States Geological Survey, was elected, April 3, a member of the American Philosophical Society, Philadelphia. Pror, JOSEPH BaArRELL, oF LEHIGH UNIversity, has been appointed assistant professor of structural geology in Yale University at New Haven. Deposits or Tin have been reported from the valley of Tuttle creek, Alaska. This stream enters the Arctic ocean a little north of Behring strait. . Proressor A. W. GRABAU delivered a public illustrated lec- ture in Boston before the Home and Field club. His subject was “Fossils, what they are and what they teach.” GEOLOGICAL SURVEY OF WASHINGTON. Governor McBride vetoed the appropriation for this survey made by the state leg- islature, thus causing its suspension for at least two years. Tur AMERICAN PHILOSOPHICAL Society has appointed a committee to prepare a plan for the appropriate celebration of the bicentennial of the birth of Benjamin Franklin, in January, 1906. - RECENT DISCOVERIES OF GOLD on the Tanana river and its tributary creeks in Alaska, are said to promise that this district will equal or exceed the Klondike district in production of gold in the near future. GEOLOGICAL SOCIETY OF WASHINGTON. At the meeting on March 11th the following program was presented: ‘“Coal- bearing series of the Yukon,” A. J. Collier; “Soils of the wheat lands of Washington,” F. C. Calkins; “Calculation of center- points in the quantitative classification of igneous rocks,” H. S. Washington; “Practical workings of the quantitative classifi- cation,” EF. B. Mathews. GEOLOGICAL Society or WaAsHINGTON. At the meeting of April 2nd the following program was presented: ‘“Correla- tion of the Potomac formation in Maryland and Virginia,” ‘Lester F. Ward; “Metallic sulphides from Steamboat Springs, Nevada,” W. Lindgren; “Origin of bedded breccias in North- ern Arkansas,’ G. I. Adams; “Dahlonega mining district, Georeia,:) Be iG. Eckel: THE TETRAHEDRAL THEORY of the outlines of the surface of the earth receives affirmative evidence in the news brought from the Antarctic by the ship Discovery. One of the angles of the tetrahedron should appear at the south pole, according to that hypothesis. Thé returning ship reports vast and moun- tainous tracts of land more or less volcanic but glacier-laden, thus greatly in contrast with the Arctic regions. ELEPHANT, Bison AND MAN IN EASTERN WASHINGTON. Dr. C. H. Sternberg in Science, March 27, 1903. recounts ex- plorations by him in 1878, in Whitman county, Washington, about 100 miles north of Walla Walla, when, in the swamps of 326 The American Geologist. Mey ee ae Pine Creek valley, he found numerous remains of elephants and bisons and came to the conclusion, from the existence of arrow points in connection with the remains, that man was cotemporary with these animals. He recommends that these swamps should be more carefully examined. In Colorado it is a remarkable fact that the profitable mines are distributed through every geological terrane, from the Archean granite to Ae Tertiary conglomerate, and mining 1s going on in rocks belonging to all the principal subdivisions Bi geological time, and abate a variety of petrographic ‘environ- ment which includes nearly all of the principal sedimentary and crystalline rocks. In arriving at the age of the country enclosing these lodes it has frequently been difficult to consider the sedimentary apart from the intrusive igneous rock, and it is not too much to say that there is not a mining district among the sixty-five which he has tabulated, in which 1eneous rocks do not occur in close association with ‘the ore deposits. T. A. RICKARD. THREE SCHOLARSHIPS of $200, $150 and $125 are an- nounced for the Harvard summer geological course in Color- ado under the direction of Mr. C. H. White. These scholar- ships are open to general application, from teachers and _stu- dents of geology, whether now enrolled at Harvard Univer- sity or not. Applications should be addressed to Mr. C. H. White, Rotch Building, Cambridge, Mass., and should describe the applicant’s previous training in geology and his purpose in further study. Letters of recommendation should be enclosed. Action on the applications will be taken June 1. The expenses of the course, including fee for instruction, will be about $200 from Chicago and return. Mr: EttswortH Huntincron has lately been appointed Research Assistant by the Carnegie Institution, and will sail April 18 with professor W. M. Davis to join professor Raphael Pumpelly in Turkestan. Mr. Huntington graduated at Be- loit college in 1897; he then spent four. years as science teach- envin Euphrates college, Harput, Turkey, and while there made an adventurous journey thro’ the canyons of the Euphra- tes, for which he has lately received the Gill memorial from the Royal Geographical Society of London. For the past two years he has been attending the Graduate School of Harvard university, and last summer he was one of professor Davis’ party in Utah and Arizona. a +, ‘ " 2: 5 “5 4 J Mie int ‘ -» , j J = » A ed : sf pa a V < 5 = : t LIBRARY cs g- “ - a7. . a a . —_ ae. HOES THES ors UNIVERSITY oF tLuioss Nag EOLOGIST, G AMERICAN THE PLATE XIX. XX XI. VOL. PaERICAN GEOLOGIST Vout. XXXI. JUNE, 1903. No. 6. JOHN WESLEY POWELL. By GEo. P. MERRILL, Washington. PORTRAIT—PLATE XIX. Major J. W. Powell, director of the Bureau of American Ethnology and for thirteen years director of the U. S. Geo- logical Survey, died at his summer home at Haven, Maine, September 23, 1902. Mr. Powell was born of English parentage in Mount Mor- ris, N. Y., March 24, 1834, his father being a Methodist clergyman. The requirements of his father’s profession neces- sitated frequent changes of home, the family moving to Jack- son, Ohio, when the subject of this sketch was about seven vears of age. When he was twelve years of age the family moved to Walworth county, Wisconsin, and again, when sev- enteen, to Illinois, in which state he remained until the break- ing out of the civil war. From early childhood Powell manifested deep interest in all natural phenomena. Original and self-reliant to a remark- able degree, he early undertook collecting and exploring trips quite unusual for a youth of his age, and studied botany, zoology, and geology wholly without the aid of a teacher. For a time in the winter of 1850 he attended school at Janesville, but much of his education seems to have been picked up at odd moments. During his residence in Wisconsin he taught school on Jefferson prairie for fourteen dollars a month, study- ing hard in the meantime and giving frequent lectures on ge- ography. After their removal to Illinois his father became one of the trustees of the college at Wheaton, and voung Powell attended the institution at intervals, teaching in the 328 The American Geologist. June, 1903, meantime at Decatur and Clinton. He also took partial courses at Jacksonville and Oberlin colleges, but was never grad- uated. He traversed various portions of Wisconsin, Illinois, Lowa, and the Iron Mountain regions of Missouri, making collec- tions of shells, minerals, and general natural history objects, which led to his election in 1859 to the secretaryship of the Illinois Natural History Society. It is said that, in 1856 when but twenty-two years of age, he descended the Mississippi alone in a row boat from the Falls of "St. Anthony to its mouth, making collections on the way. Again, in 1857, he rowed the whole length of the Ohio river from Pittsburg to its mouth, and in 1858 made a like trip down the Illinois river to its mouth and thence up the Des Moines. : With the outbreak of the civil war Powell enlisted in the 20th Illinois volunteers, and was mustered in as second leu- tenant. He was for a time stationed at Cape Girardeau and as captain of battery F of the 2nd ‘Illinois artillery took part in the battle of Shiloh, losing his right arm at Pittsburg Land- ing. He returned to the service as soon as his wound healed, and took part in the battles of Champion Hill and Black River Bridge. At the close of operations about Vicksburg he was obliged to submit to a second operation on his arm, but returned to his post in season to take part in the Mer- idan raid. Later he was made major and chief of artillery, first, of the 17th army corps and subsequently, of the depart- ment of Tennessee, taking part in the operations before At- lanta and in the battle of Franklin. At the close of the war he accepted the position of profes- sor of geology and curator of the museum of the Illinois Wesleyan University at Bloomington, from which institution, although not a graduate, he had previously received the de- erees of A.B. and A.M. He also became connected with the Illinois Normal University and was widely known through- out the state by his lectures and addresses on scientific sub- jects. In May, 1867, Powell visited the Rocky mountains of Colorado, taking with him a party of sixteen students. This was before the completion of the Pacific R. R. and when the country was still infested by Indians. The party ascended John Wesley Powell—Merrill. 329 Pike’s peak and mount Lincoln. After the breaking up of the party at Denver, major Powell and his wife, who had accompanied him, visited Middle park of Colorado and con- tinued their explorations until snow interfered. In 1868 Powell organized a party for the purpose of a second expedition into Colorado, finally going into winter quarters on the White river. During this trip he made im- portant studies in high altitudes, ascending Long’s peak for the first time and traversing a considerable portion of the mountain system of Colorado: In the summer of 1869 he organized an expedition for the purpose of exploring the Grand Canton of the Colorado itself, a region up to this time almost wholly unknown and con- cerning which there were many vague and often wild rumors. The party, consisting of eleven men with four boats and pro- visions for ten months, started on its voyage on May 24 and emerged from the mouth of the Grand Cafion August 29 following, having made a journey of nearly goo miles and one which has been described as unequaled in the annals of geographical exploration for the courage and daring dis- played in its execution, The immediate geological results of this trip were very slight. Nevertheless, the prestige gained was such as to be of great benefit to Powell throughout his en- tire career. Explorations of the cahon and adjacent regions were con- tinued during 1870, 1871, and 1872, the results being pub- lished in 1875 under the caption of Explorations of the Col- orado River of the West and its Tributaries, in form of a quarto volume of nearly 300 pages, It was in the second part of the report, relating to the physical features of the valley of the Colorado, that Powell called attention to the fact that: the Uintah cafions were gorges of corrosion and due to the action of rivers upon rocks which were undergoing gradual elevation. As he expressed it, the river preserved its level, but the mountains were lifted up, as the saw re- volves on a fixed pivot, while the log which it cuts is moved along, the river being the saw which cuts the mountain in two. This, it will be remembered, was essentially the idea advanced by Hayden with reference to the cafions of the Yellowstone, Madison and Gallatin in his report on the geol- 330 The American Geologist. June, 1903. ogy of Montana (1872, p. 85). In this same report Powell first made use of the expressions antecedent and consequent with reference to valleys, meaning, in the first instance, that the drainage was established prior or antecedent to the cor- rugation of the beds by faulting and folds, and in the sec- ond case, that the valleys had directions which were de- pendent upon the corrugations. Valleys which were formed by streams, the present courses of which were determined by conditions not found in the rocks through which the chan- nels are now carved, and which were in existence when the district last appeared above the sea-level, he called super- imposed valleys. He also here used for the first time the term base level of erosion, which he defined as “an imagin- ary surface inclining slightly in all its parts toward the end of the principal streams draining the area through which the level is supposed to extend, or having the inclination of its parts varied in direction as determined by tributary streams.” He pointed out, also, that the region of the Grand Canon was, after all, the region of less rather than greater erosion; that, had the country been favored with a rainfall equal to that of the Appalachian country, the entire area hight have been reduced to a base level which would be the level of the sea, though the evidences of such erosion might be almost wholly obliterated. In 1871, 1872, with the aid of a Government appropria- tion of twelve thousand dollars, the organization known as the Survey of the Rocky Mountains was established, in rivalry with those of Hayden and Wheeler. At the head of this Powell remained until the three were abolished in 1879 and the U. S. Geological Survey created, with Clarence King at its head. It was while carrying on this survey that G. K. Gilbert was detailed to study the Henry mountains in Utah, the results of which were brought out-in the now clas- sic monograph relating to the Laccolithic Mountains, Powell’s first observations on the geology of the Uintah mountains were made in 1869. In 1871, 1874, and 1875 he again personally visited the plateau region, the last time be- ing accompanied by Dr. C. A. White. The results of these later years of exploration are given in the quarto monograph On the Geology of the Eastern Portion’ of the Uintah Moun- John Wesley Powell.—Merrill. 26 tains, which was published in 1876. In this, as in all the work of the Powell surveys, little or no attempt was made at systematic areal geology; certain striking and well-ex- emplified features were selected and made the subject of special monographs. In the work above noted Powell e Xs $4125 SLEBANO ~ oR n> ©\ Crab Orchard SCALE — 10 15 20 ooh SS es es fH John Wesley Powell—Merrill. 333 Although himself not a college graduate, Powell received in 1886 the degree of Ph.D. from Heidelberg, Germany, and and that of LL.D. from Harvard. In 1862 he married Miss Emma Deane of Detroit. His widow and one daughter sur- vive him. THE RICHMOND GROUP ALONG THE WESTERN SIDE OF THE CINCINNATI ANTICLINE IN INDIANA AND KENTUCKY. By AuG. F. FoERSTE, Dayton, Ohio. PLATES XX-XXH. CONTENTS. A. Thesubdivisions of the Cincinnati Series..............:. sence 333 The Mount Acwburd Ded sie. -. <3... aca ese iewnewnlc arcane ecvee 334 MSE WVEV Greta De Occacce ecee hese sources cs cataswenacsnadstcawasscavesne 335 The base of the Lower Richmond..... ..... .......s0ee00. 336 The top of the Lower Richmond...........6...2---.ssssesee 339 Aine WMincd GLE 1G aTlOMdrsssssteestenensreccssrecassecences mst crnnes 340 The base of the Upper Richmond. ...................seeeeees 34.2 The top of the Upper Richmond.....-...---.-... cesses eeeee 346 B. Decrease in thickness of the Richmond group...........-.- 34:8 Hees Mernicl eal tcsee ee ae dae axest teem ee tencit c= se asia cue otine ysinislsenals vie stag 348 AEG RACH i116 Mle Stele manson ss sere aceite =e-lasess) eas eerine 348 The Middle and Lower Richmond............-.464- 348 TOD CCIE CK Yjae ones cellar eiawesecswecs own deve cece caatiarlestewice esas 349 Nhe RACIMUOMG SEA REy. case meee =n eines tame sn SPOTS COOINS 349 The Middle and Lower Richmond.................. 350 Coral reefs in Kentucky and Irdiana............ 352 The Upper Richmond............:..-esecesssss scenes eseeee 354 ee CONCUSSIONS ener ee ree tees teeter oreen cena «sere amemaeaaawatssinetes 354 A: THE SUBDIVISIONS OF THE CINCINNATI SERIES. In Ohio, that part of the Ordovician system which overlies the Trenton is included in the Cincinnati series. The Cincin- nati series is divided into three stages of nearly equal thickness : the Richmond stage, which attains a thickness of about 235 feet along its northern line of outcrop in Indiana and Ohio; the Lorraine stage, 300 feet thick; and the Utica stage, 260 feet thick. The various subdivisions of these stages* are given in the following table, in descending order :— *“The Geology of Cincinnati,’’ J. M. NICKLES, Jour. Cincinnati Soc. Nat. Hist., 1902, No. 2. The writer is much indebted to this paper, and also to many suggestions given personally by Mr. Nickles, in the field and elsewhere. The writer accompanied Mr. Nickles on a trip during which the localities between Versailles and Marble Hill were visited. June, 1908. 334 The American Geologist. Saluda, Madison, or Upper Richmond bed, 60 feet. Middle Richmond, 115 feet. Lower Richmond, - 60 feet. Warren bed, 70 feet. Mount Auburn bed, 20 feet. Monrainevstacies seme Corryville bed, 60 feet. Bellevue bed, 20 feet. | Fairmount bed, 80 feet. (| Mount Hope bed, 50 feet. Upper Utica, 60 feet. iicarstaceyen ene aes Middle Utica, 120 feet. Lower Utica, 8o feet. The Mount Auburn Bed. The Mount Auburn bed is characterized by the presence, in great numbers, of a large, globose form of Platystrophia lynv,t with a hinge-line considerably shorter than the width of the shell. This globose form may be regarded as a senile, gerontic variation of a second, equally large form having a much greater vertical range. In the second form the hinge line equals or slightly exceeds the width of the shell, thus giv- ing the shell a more quadrate outline. In Ohio, a few stray specimens of the large quadrate form are seen in the Fair- mount, Bellevue, and Corryville beds; they occur most abund- antly, associated with the gerontic specimens, in the Mount Auburn bed; and they are found in the Morris Hill section, three miles northwest of Oregonia, in the Warren bed, forty feet above the Mount Auburn bed. In many parts of Ken- tucky, especially east of the Cincinnati anticline, the quad-ate form has about the same vertical range, namely from the Fair- mount to the Warren beds, but it is much more abundant in the lower beds there than in Ohio. In Kentucky, therefore, the name Platystrophia lynx bed includes a large part of the Lor- raine, while in Ohio the name is restricted to the Mount Au- burn bed, which is characterized by the presence of numerous senile or gerontic specimens. In the upper part of the Mount Aubtirn bed at Madison, Indiana, a species of Plectorthis occurs which resembles Plect- * Paleozoic seas and barriers, ULkKICH and SCHUCHERT, Report, New York State Paleontologist, 1901 (Published in 1902), p. 643. ; } “The Morphogenesis of Platystrophia,’’?’ E. R. CUMINGS, Am. Jour. Sci., 1903, p12, 26. { Tbid.; p. 19,24. Richmond Group of Cincinnati Anticline.-—Foersie. 335 orthis fissicosta as figured by Meek.* The area of the ventral valve is large, forming an angle of about seventy degrees with the plane separating the valves. The convexity of the ventral valve however is much less; the shell has a flattened appear- ance anterior to the beak, and is often slightly depressed near the middle of the anterior margin, giving a slightly sinuous outline to this part of the shell. There is also a greater in- equality in size between the plications originating at the beak and those added later, so that the earlier formed plications are more conspicuous along the anterior half of the shell. The same form occurs in the Corryville bed at Cincinnati, Ohio, where it is identified as Plectorthis dichotoma. Plectorthis fissicosta of Meek, from the Fairmount beds at Cincinnati is also identified as Plectorthis dichotoma, by Schuchert.+ ‘The Corryville and Mount Auburn specimens just described may be easily distinguished from the Fairmount specimens now re- ferred to Plectorthis dichotoma., The Warren bed. The most characteristic brachiopod of the Warren bed is Dinorthis retrorsa: it is restricted, however, to a very short vertical range near the middle of the bed. Along the creek directly north of Lebanon, Ohio, a coarse limestone layer, four inches thick, occurs thirty-three feet above the Mount Auburn bed. The limestone layer is found at the north end of a large exposure on the west side of the creek, near the base. Three feet above this layer, Dinorthis retrorsa occurs associated with Leptaena rhomboidalis. Specimens of Dinorthis retrorsa were collected also eight feet above the limestone layer; the vertical range is therefore five feet. About seven miles northeast of Lebanon, Cesar’s creek flows into the Little Miami river from the east. Almost di- rectly opposite, Lick run enters the river from the west. Lick run has its source in a spring located on the northeast side of a rise of land, formerly known as Morris hill, about two miles west of the river. The section along Lick ran was used by professor Orton to determine the thickness of his Lebanon beds, which included both the Warren and the Richmond beds. The Mount Auburn bed is not exposed here. The large, quad- * Pal. Ohio, vol.i, 1873, pl. 8, fig. 6. + Synopsis of American Fossil Brachiopoda, p. 312. 330 The American Geologist. sees rate form of Platystrophia lynx is rather common in a layer of limestone occurring thirty-four feet above the level of the river. Three feet farther up, there is a coarse limestone layer, its upper surface strongly wave-marked, the trend of the ridges approximately north and south. Three and a half feet above the wave-marked layer, Leptaena rhomboidalis occurs. Four feet above the wave-marked layer, Dinorthis retrorsa is rather common, and its range extends fully six feet above this level. Above the Dinorthis retrorsa layers, in the Lebanon sec- tion, there is blue clay, sixteen feet thick, soft near the base, nodular near the top. Overlying the clay is nodular clayey limestone, three and one-half feet thick, which may be regarded as forming the top of the Warren bed. The topmost layer is wave-marked in places, the trend of the ridges being approx- imately north and south. The nodular character of the rock and the wave-marking suggest turbulent waters during the de- position of the upper Warren beds. This was followed by a change of fauna inaugurating the Richmond age. The base of the Lower Richmond. Zygospira kentuckiensis has been found in Oldham and Jefferson counties in Kentucky, and at the mouth of Bull creek, in the northeastern part of Clark county in Indiana. At the last named locality it occurs at the contact of the Lorraine with the Lower Richmond. At Clarksville, Ohio itt occurs in the upper part of the Lower Richmond, about four feet below the horizon of Herbertella insculpta. | The nodular, clayey limestone at the top of the Warren bed,. in the Lebanon section is overlaid by thin, well bedded lay- ers of clay and limestone; the total thickness is four feet; the top is formed by a four inch layer of hard limestone. Immedi- ately above, in the blue clay and in the interbedded thin lime- stone layers, Dalmanella jugosa is common, Nine feet above the Warren bed there is a more massive layer of limestone,. four to nine inches thick, containing great numbers of this fossil. In the gulley back of the blacksmith shop, at the north end of Oregonia, a station formerly known as Freeport, Dinorthis retrorsa occurs seventy-eight feet above the level of the river. The base of the nodular clayey limestone occurs sixteen feet. Richmond Group of Cincinnati Anticline—Foerste. 337 above this level. The lower part, a foot and a half thick, is more connected; the upper part, three and a half feet thick, consists of nodular limestone masses more or less separated by clay. This forms the top of the Warren bed. Five feet above this level Dalmanella jugosa occurs in a very clayey limestone. A layer of hard limestone containing great numbers of this fossil is found seven feet higher up. The upper range of this fossil is not well exposed here. Two miles south of Oregonia, on the main road from Leb- anon to Wilmington, Dinorthis retrorsa occurs ninety-one feet above the level of the railroad, at a little stone culvert, just north of the bend where the road ascending the hill turns ‘sharply eastward. The top of the Warren bed is twenty-one feet farther up, and five feet higher Dalmanella jugosa occurs in a clayey nodular limestone. It is much more abundant in the clays and thinbedded limestones immediately above, and has a range of at least fifty feet. At this locality the lowest specimens of Strophomena rugosa were found in the upper part of the Dalmeanella jugosa zone. Along its northern line of outcrop in Ohio and Indiana, the lower part of the Lower Richmond is characterized -by the great abundance of Dalmanella jugosa. While at several lo- calities this species appears to occur in small numbers in the upper, nodular part of the Warren bed, its increase in the low- er part of the Lower Richmond is so abrupt that it is one of the most useful fossils for determining the line between the War- ren and the Lower Richmond. Southward the Dalmanella jugosa zone thins out. While very abundant at Concord, Ken- tucky, no traces of this fossil were seen at Owingsville or near Spencer. On the western side of the Cincinnati, anticlin<, it has not been seen south of Marble Hill in Indiana. The most southern outcrop of Dinorthis retrorsa.on the eastern side of the Cincinnati anticline is at Arnheim, in Brown county, thirteen miles north of the Ohio river. Dal- manella jugosa and Hebertella insculpta are common at Con- cord, Kentucky. Catazyga headi occurs ten miles south of “Maysville, Kentucky. Protarea vetusta, Streptelasma rusticum (Str. corniculuim of the Ohio survey), Strophomena sulcata, and Rhynchotrema capax range from the lower part of the Lower Richmond to 338 The American Geologist. Daa ete" the top of the Upper Richmond. Since they are not known to occur in the Lorraine in the area under discussion, these spec- ies are very useful for distinguishing between the Lower Rich- mond and the Warren beds in those parts of Indiana and Ken- tucky in which the Dalmanella jugosa zone is absent. Usually they are rather infrequent in the lower and middle part of the Dalmanella zone and do not become abundant until the upper part of this zone is reached. Strophomena rugosa (Str. planumbona of the Ohio Sur- vey) is another Richmond fossil which usually does not be- come abundant until the middle or upper part of the Dalman- ella jugosa zone is reached. The radiating striz are of medi- um size, and do not differ conspicuously in size either when strie on the same valve, or when striz belonging to opposite valves are compared. Strophomena elongota James, is a variety of Strophomena rugosa, differing only in the greatly extended hinge-line, which gives a subtrig- onal, instead of the usual subquadrate outline to the shell. Strophomena subtenta (Str. plicata of the Ohio Survey) 1s another variety, of larger size than the typical Str. planwm- bona; the oblique wrinkles near the extremities of the hinge- line are often absent. Strophomena elongata and Str. subtenta are typically developed in the lowest part of the Middle Rich- mond. Forms intermediate between these varieties and Str. planumbona occur in the upper part of the Lower Richmond. Strophoniena neglecta has been collected by Dr. G. M. Austin in the upper ten feet of the Lower Richmond near Clarksville, Ohio. It is a larger shell than Str. vetusta, often attaining a width of 50 mm. The convexity of the dorsal valve is much greater, the depth amounting to 1.8 mm. in shells 42 mm. long. The striz are much finer and closer over the larger part of the shell, and equal in coarseness those of the dorsal valve of Str. vetusta only along the anterior third of the shell. The chief characteristics of Strophomena nutans are its subnasute anterior margin and the remarkable thickening of the interior of the ventral valve around the muscular area and along the anterior margin. The radiating strie are very fine; some, at more or less regular intervals are slightiy more prominent. The typical specimens are rather small, mature spec- imens attaining a length of four-fifths of an inch. They oc- 7 _— Richmond Group of Cincinnati Anticline-—Foerste. 339 cur in the middle and upper part of the Lower Richmond. At Concord in Kentucky, specimens having the same general form as Strophomena nutans are found at the base of the Dal manella jugosa zone, eighteen feet below the lowest specimens of Strophomena rugosa. Many of these specimens attain —a length of one inch and a width along the hinge-line of an inch and a quarter. The striz of both valves are fine; some are more prominent, three to six intermediate striz being less conspicuous. About six to nine of the more prominent striz eccur in a width of a quarter of an inch. The top of the Lower Richmond. At the bridge across Todd’s Fork, northwest of Clarksville, Ohio, Dalmanella jugosa occurs sparingly in the clayey lime- stone at the base of the section. Immediately above, it be- comes very common, and remains common as far as forty to forty-three feet above the level of the creek. Forty feet above the creek there is a wave-marked layer of limestone, with the ridges trending approximately northeast and southwest. Fifty feet above the creek, Hebertella insculpta is rather common, but is restricted to only a few feet in the vertical section. Dal- manella jugosa occurs sparingly up to this level, and even for five or more feet above the same. The Hebertella insculpta horizon may be regarded as form- ing the top of the Lower Richmond. It has not yet been defi- nitely determined that this fossil is restricted to the top of the Lower Richmond, but it is known at least to be quite constant in its appearance at this horizon in northeastern Kentucky, all of Ohio, and in Indiana as far south as Weisburg and Ver- sailles. It may be that it occurs as far south as Madison but no specimens have been collected there. At Versailles, in Indiana, Rynchotrema dentatum makes its first appearance in the Lower Richmond at a level one or two feet beneath that of Hebertella insculpta. At Dayton, Ohio, and at Richmond, Indiana, its range extends to the top of the Middle Richmond. While it is not known to occur in the lower part of the Lower Richmond, a very similar, if not identical form has been found in the upper part of the Warren bed half a mile southeast of Howard’s mill in Montgomery county, Kentucky. It possesses three distinct plications and one indistinct plication on each side of the dorsal fold instead of 340 The American Geologist. June..190e. four distinct and one or two indistinct plications, as in the Richmond group. In consequence, the plications appear more angular. A single specimen of the Warren bed form was col- lected by Mr. J. F. Hammel at Madison, Indiana, but the exact horizon from which it was collected is unknown. Catyzyga headi may prove to be a very valuable horizon marker.’ It appears to have a very restricted vertical range. At Clarksville, Ohio, it has been collected, by Dr. George M. Austin, anout fifteen feet below the horizon of Orvthis insculpta. Lower down along Todds Fork, in Warren county, it has been collected by the same observer at the same level, near the hill tops about Hicks station. At Madison, Indiana, where the Hebertella insculpta horizon is unknown, Catysyga headi is found fifty feet above the base of the Richmond. This must be somewhere near the top of the Lower Richmond. Dinorthis scovillei has so far not been found outside of the limits of Warren county, Ohio, although it is a well character- ized species. This is probably due to its very limited vert'cal range. On Longstreth’s creek, west of Oregonia, it occurs at about the same level as Gawrocrinus nealli, a short distance below the Dendrocrinus caduceus horizon, and a greater dis- tance below the Hebertella insculpta horizon. Dalmanella jugosa occurs farther down the creek. The type of Lingula vanhornei was found in the Lower Richmond, at Versailles, Indiana. The Middle Richmond. Dinorthis subquadrata, Hebertella occidentalis, Platystro- phia acutilirata, and Strophomena vetusta (Str. flitexta of the Ohio survey) make their first appearance in the Middle Rich- mond and are therefore very serviceable in distinguishing the middle Richmond from the Lower Richmond in the areas in which Hebertella insculpta is absent. Dinorthis subquadrata, Hebertella occidentalis, and Platystropma acutilirata occur al- so in the fossiliferous horizons of the Upper Richmond. Typi- cal specimens of Hebertella occidentalis occur along Elkhorn creek near Richmond, Indiana, twenty-seven feet below the Clinton. Forms with only a moderate depression along the middle of the dorsal valve occur in the upper beds as far as the base of the Richmond. Richmond Group of Cincinnati Anticline.—Foerste. 341 Platystrophia acutilirata is a descendant of Platystroplua laticosta. The typical specimens of Platystrophia laticosta begin their appearance in the Bellevue bed, and thence continue through the remainder of the Lorraine stage into the Lower Richmond. In the Lower Richmond a part of the spec- imens show an increase in the number of lateral plications and a prolongation of the postero-lateral angles, features which find their most pronounced expression in Platys- irophia acutilirata. Platystrophia cypha from the Lower Richmond, is evidently one of the transitional forms in which the increase in the number of. lateral plications and the prolongation of the postero-lateral angles has been accom- panied by a reduction in the number of plications on the me- dian fold and in the sinus. Strophomena planumbona occurs in the middle part of the Lower Richmond. Strophomena subtenta is found in the lower part of the Middle Richmond. Specimens intermediate between Strophomena planumbona and Strophomena subtenta are found in the upper part of the Lower Richmond In typical specimens of Strophomena subtenta the thick- ening of the border around the anterior and lateral mar- gins of the interior of the shell is comparatively small, the muscular cavity is less prominently bordered, and the shell attains a larger size. The posterior.half of the dorsal valve is distinctively flattened and usually slightly concave anterior to the beak. The striations of the.ventral valve are about equal in size to those of the dorsal valve. Strophomena vetusta differs from Strophomena sub¢enta in the much smaller and more even convexity of the dorsal] valve, and in the very slight flattening of this valve near the beak. The radiating striations of the ventral valve are conspicuously finer than those of the dorsal valve. Moreover, the radiating striations of the ventral valve are crossed by fine concentric striations and wrinkles which are usually readily seen, especially on the posterior half of the shell, and are very characteristic of this species. As a rule, the cardinal area of the ventral valve is much higher at the beak in Strophomena vetusta than in Strophomena subtenta. 1 am under great obligations to pro- fessor Stuart Weller for the opportunity of examining the type specimens of Strophomena vetusta in Chicago University. 342 The American Geologist. June, 1903. They were found at Blanchester, Ohio, in the Middle Rich- mond. The wrinkling of the shell along the hinge-line is scarcely a specific character, and may be absent. Strophomena vetusta makes its first appearance in the lower part of the Middle Richmond and is usually abundant in the middle and upper part. Strophomena approximata is a subtrigonal form of Str. vetusta, The type specimens were found in Dearborn county, Indiana, in the Middle Richmond. All of the exposures in the immediate vicinity of Richmond, Indiana, belong to the Middle Richmond. The base of the Mid- dle Richmond is not seen. Strophomena subtenta occurs only at the very base of the exposures, while Strophomena vetusta occurs at all levels. At the top of the exposures Strophomena sulcata 1s rather frequent. The base of the Upper Richmond. Along the northern line of outcrop, in Ohio and Indiana, the richly fossiliferous clays and limestones of the Middle Richmond are followed by a considerable thickness of clays in which fossils are much less abundant or even absent. These upper clays are referred to the Upper Richmond. Farther south, in the vicinity of Laurel, Indiana, the equivalent beds consist of a nearly unfossiliferous clay rock, forming steep walls at the base of several waterfalls but disintegrating read- ily under the influence of weathering. At Madison, the equiv- alent beds consist of an earthy, siliceous limestone which is harder than the clay rock at Laurel and is well bedded so that at one time it was quarried. Its appearance, however, has proved to be deceptive, and this rock is now known to be strongly affected by weathering. The main body of this rock at Madison does not contain fossils and elsewhere it usually contains so few fossils that its geological position long re- mained unknown. Upon lithological grounds it has been re- ferred in former times to the Silurian, but an unmistakable Or- dovician fauna is now known from the body of this usually nearly unfossiliferous sectien, and an abundant Ordovician fauna overlies it at Madison. | The separation of the Upper Richmond from the Middle Richmond must usually be effected by lithological means. The Middle Richmond consists of a series of richly fos- Richmond Group of Cincinnati Anticline.—Foerste. 343 siliferous limestones interbedded with richly fossiliferous clays. The Upper Richmond consists of much less fossilifer- ous material, varying geographically from soft clay to clay rock and to massive beds of argillaceous limestone, fairly hom- ogeneous throughout the greater part of the vertical section. In the vicinity of Madison, Indiana, the more massive, banded, argillaceous limestone is thirty-two feet thick. At its base and also higher up in the series, some of the layers show ripple marks and sun cracks. Beneath this, the rock is softer, more clayey, disintegrates more readily, often forming a clay- ey section, fifteen to seventeen feet thick. The base of the clay- ey section is formed by a layer, one or two feet thick, which evidently at one time formed a thin coral reef. Massive spec- imens of Columnaria alveolata (Favistella stellata of the Ohio and Indiana surveys), and Columnaria halli (C. alveolata of -most authors of former days) are very common. Many of the specimens form masses six inches thick and twelve inches broad. A few are a foot and a half thick and nearly three feet broad. Specimens of Calopoecia cribriformis are rather scarce. Occasional specimens of Tetradium minus are found. The last named fossil occurs also in layers six feet, and seven and a half feet above the coral bed, and in a layer two feet below this bed. This coral bed may be traced southwestward as far as Han- over, and northeastward as far as the northern part of Jeffer- son county. Stray specimens of Columnaria alveolata have been found at the same horizon as far south as the D. P. Mon- roe locality, one mile northwest of the Pinckney Swan locality, and as far north as Versailles. At Versailles, Tetradium minus occurs at all levels in the thirteen feet which overlie the layer containing Colwmnaria alveolata. It is quite abundant in about nine feet of the sec- tion. The base of the Tetradium bed at Versailles is, therefore, approximately at about the same level as the coral bed at Mad- ison. This is believed to be the case also at Laurel, where no Columnaria has been found, but where a Tetradium minus layer, three to four feet thick, occurs at a corresponding level. At Richmond, Indiana, small specimens of Columnaria alveo- lata and Columnaria halli, not exceeding two inches in diameter, occur associated with Beatricea undulata on Elkhorn creek fif- 344 The American Geologist. Tune, 2808. teen feet below the Clinton. In the valley of Whitewater river John Misner found two specimens of C. alveolata near the base of the Middle Richmond, and two equally large specimens of Calopoecia cribrifornus were found, one near the base and the other near the top of the Middle Richmond. Wherever, in Indiana, the horizon of the coral reef exposed at Madison can be determined, or wherever Tetradium minus forms a well marked zone at practically the same horizon, the base of these beds is considered the paleontological base of the Upper Richmond. A great coral reef, made up of numerous specimens of Columnaria alveolata, Columnaria hall, and Calopoecia cribni- formis is found also in central Kentucky, in Nelson, Marion, and Washington counties. It occurs at the base of the Rich- mond section as exposed in that part of the state. This coral bed in central Kentucky probably was not synchronous with the coral bed in southern Indiana. Although the lower and middle beds of the Richmond stage thin out rapidly southward, so many Middle Richmond fossils occur in the lower part of the Richmond section in central Kentucky, just above the coral. bed, that it seems probable that the coral reef of central Ken- tucky is of earlier date than the coral reef at the base of the Upper Richmond in southern Indiana. While the base of the Upper Richmond at many localities in southern Indiana is characterized by the presence of numer- ous specimens of Colummnaria alveolata, Columnaria halli, Cal- opoecia cribriformis, and Tetradium minus, none of these fos- sils are confined to this horizon.* Columnaria alveolata occurs in the Black River limestone of Ontario, and in the Trenton formation of Manitoba and of the district of Mackenzie. It is found at the top of the Lor- raine, associated with Dinorthis retrorsa, at Clifton, Tennessee. Small specimens, three inches in diameter, occur above He- bertella insculpta at Concord, Ky. Small specimens are found also in the lower half of the Middle Richmond, on East Fork of ‘Ludds Fork, Ohio, and fifteen feet below the base of the Clin- * “A revision of genera and species of Canadian paleozoic corals,’’ L. M. LAMBE, 1901. pp. 43. 90, 93, 98, 100, 110. The Cincinnati Group in Western Tennessee, Journal of Geology, 1903, p.37: 2 7 : “Corals from the Lower Silurian of Minnesota,’’ Geology of Minn.,, vol. iii, part 1, WINCHELL and SCHUCHERT, pp. 85, 93, 94. Richmond Group of Cincinnati Anticline.—Foerste. 345 ton in the valley of Elkhorn creek, near Richmond, Indiana. Two large specimens were collected by John Misener near the base of the Middle Richmond, at Richmond, Indiana. Columnaria halli is typical of the Birdseye and Black river formations in Quebec and Ontario. It occurs in the Black River group of New York. It is found in the Trenton of Min- nesota, Wisconsin, Illinois, Kentucky, and central Tennessee. It is abundant in the Upper Lorraine at various localities in Bul- litt, Nelson, and Marion counties in central Kentucky, associ- ated with Beatricea undulata. One specimen referred to this species was collected above the Hebertella insculpta zone at Concord, Kentucky. It occurs about eighteen feet below the top of the Lower Richmond near Clarksville, Ohio, and also twenty feet above the base of the Middle Richmond in Roar- -ing run, in Warren county. Along Elkhorn creek near Rich- mond, Indiana, small specimens occur fifteen feet below the base of the Clinton. Calopoecia cribriformis is probably identical with Cal- Opoecia canadensis. It occurs in the Birdseye near Otta- wa; in the Black river at the north end of lake Huron, in the province of Quebec, and on Anticosti; in the Galena- Trenton in Manitoba and in the district of Saskatchewan; and in the socalled Hudson river of the northern end of lake Hur- on, in the province of Quebec, and on Anticosti. It occurs in beds which may belong to the top of the Lorraine at the Lang Smith locality, a mile and a half southeast of Chicago, in Ken- tucky, and at the home of George Raley, 3 miles southeast of Lebanon, Kentucky. It has been found by Dr. G. M. Austin at the top of the Lower Richmond, in Cowais creek near Clarks~ ville, Ohio. Two specimens were collected by John Misener at Richmond, Indiana, one near the top and the other near the bot- tom of the Middle Richmond. Tetradium minus is probably identical with Tetrudium fibratum. These forms range from the Birdseye and Black River formations in Canada, to the Galena-Trenton in Man- itoba; and to the Trenton in Kentucky and Tennessee. Tet- radium minus occurs at the top of the Lorraine near the mouth of Bull creek, in Clark county, Indiana. In southern Indiana, Ohio, and Kentucky, it is common at the top of the Upper Richmond. 340 The American Geologist. June, 1903. The chief thing which is characteristic of the occurrence of these corals at the base of the Upper Richniond in southern Indiana is their great abundance and large size at this partic- ular horizon, indicating the presence of a coral reef. This coral reef is occasionally followed at intervals of several feet by other beds in which the same species of corals occur, but in these beds the corals are less numerous and usually much smaller. Elsewhere in Indiana and Ohio these corals occur only as occasional specimens not forming reefs. Along Elkhorn creek, four miles south of Richmond, the highest exposures containing Strophomena vetusta, Dinorthis subquadrata, Rhynchotrema dentata, and Strophomena_ sul- cata occur between fifty and sixty feet below the Clinton. The upper beds of the Richmond are more richly fossiliferous along Elkhorn creek than at any other locality in Indiana and Ohio, so far examined. The top of the Upper Richmond. At most localities almost the entire Upper Richmond sec- tion is unfossiliferous. The coral bed and the layers immedi- ately above often contain a few fossils. At Madison, a whitish band of calcareous rock six feet above the coral bed contains Cyrtolites ornatus, Bellerophon mohri, Lophospira bowdeni, Hormotoma gracilis, Ischyrodonta miseneri, and a small vari- ety of Platystrophia* three quarters of an inch in width, the hinge line scarcely exceeding the general width of the shell. In the sandy layers immediately, above, Rhynchotrema capax, Strophomena sulcata, Hebertella sinuata, and large, branching, nodular specimens of Heterospongia aspera are found. In the southern half of Ripley county, in Indiana, the middle part of the Upper Richmond section contains a considerable bryozoan fauna, although the number of species is apparently small. Hebertella sinuata and Byssonychia radiata are fairly common. Near Versailles the upper part of the Upper Richmond con- sists of sandy clay containing in addition to numerous speci- mens of bryozoa, also Streptelasma rusticum, Protarea vetusta, Flebertella occidentalis, Strophomena sulcata, and the small Platystrophia with a short hinge line, which occurs also lower in the section. Along Elkhorn creek, four miles south of Rich- *“The Morphogenesis of Platystrophia,’’ E. R. CUMINGS, Am. Jour. Sci., 1908, p. 25. Richmond Group of Cincinnati Anticline.—Foerste. 347 mond, Indiana, the Upper Richmond is richly fossiliferous. Bucania crassa occurs associated in the various species of /s- chyrodonta, seven feet below the Clinton. Helicotoma margin- ata is found associated with Beatricea undulata fifteen feet be- neath the Clinton. It is evident that, notwithstanding the gen- eral scarcity of fossils at most exposures of the Upper Rich- mond, continued search will reveal a considerable fauna. Most of the forms so far identified seem to occur also in the Middle Richmond, but when the bryozoans are studied it is probable that a number of species will be found restricted to this upper subdivision of the Richmond stage. At Madison, Indiana, fossils are found in the thin clayey partings between the upper layers of the massive banded argil- laceous limestone. Immediately above are several feet of fos- siliferous clay and fine grained, dense, bluish limestone. These contain, in addition to fossils found also in the Richmond beds beneath, a few fossils which are apparently typical of this hori- zon. Among these are Cyrtocerina madisonensis, Lophospira hammelli, and a species which was described as Holopea hub- bardi, but which probably belongs to some undescribed genus. Labechia ohioensis, Labechia montifera, Tetradiuim minus, and various species of ostracoda are common at some localities, but ure found also at lower horizons elsewhere. In the reports of the Indiana survey, the beds at the top of the Ordovician sec- tion at Madison are referred to as the Murchisonia hammelli beds,* or as the gasteropod layer. Since the most varied fauna so far obtained from this horizon was collected in West Madi- son along the brow of Hitz hill, on the western side of the Madison branch of the Panhandie railroad, the bed may also be called the Hitz bed. The most southern exposure of this bed so far seen is located about ten miles southwest of LaGrange, near Floydsburg, Kentucky, on the Alexander Sinclair farm. The most northern locality known is found two miles north of the southern boundary of Ripley county, four miles west of Cross Plains, Indiana. The distance between the extreme points named is nearly fifty miles. 348 The American Geologist. piers B. DEcREASE IN THICKNESS OF THE RICHMOND GROUP. I. Indiana. The Richmond stage. At Fort Recovery,* in the southwestern part of Mercer county, Ohio, a bed of fossiliferous limestone was struck in a gas well, at a level of 270 feet beneath the Clinton. The fos- siliferous limestone continues for a depth of thirty feet. The rock is almost entirely made up. of Dalmanella jugosa. The thickness of the Richmond stage at Fort Recovery is therefore about 300 feet. From this point southward, as far as Raywick, in the western part of Marion county, Kentucky, a distance of 200 miles, the Richmond stage becomes constantly thinner. 3etween Fort Recovery, Ohio, and the Brookville-Laurel section, in Indiana, a distance of seventy miles, the thickness of the Richmond diminishes from 300 to 250 feet, an average diminution of .7 foot per mile. Between Brookville (250 feet) and Versailles (217 feet), a distance of thirty miles, the aver- age diminution in thickness is 1.1 feet per mile. Between Ver- sailles (217 feet) and Madison (178 feet), a distance of twen- ty-five miles, the average diminution is 1.6 feet per mile. Be- tween Madison (178 feet) and Hanover (169 feet), a distance of five miles, the average diminution is about 1.8 feet per mile. Between Hanover (169 feet) and the Pickney Swan locality on. ‘Saluda creek (440 feéet){, a. distance: of fiver oniles: the average diminution is about 5.8 feet per mile. Be- tween Saluda creek (140 feet) and Marble Hill (111 feet), a distance of 3.5 miles, the average diminution is 8.3 feet per mile. Between Marble Hill (111 feet) and the mouth of Pull creek (83 feet), a distance of eleven miles, the average dimin- ution of the Richmond stage is 2.5 feet per mile. The Middle and Lower Richmond. As far south as Hanover, Indiana, Dalmanella jugosa is very abundant at the base of the Richmond stage, its range extending through the greater part of the Lower Richmond. At the Pinckney Swan locality on Saluda creek, it is abundant only in a few feet of rock at the base of the Richmond sec- tion. At Marble Hill, a few specimens were found in the few inches of sandy limestone at the very base of the Richmond * Geology of Ohio, vol. vi, 1888, p. 263. THE AMERICAN GEOLOGIST, VOL. XXXI. PLATE XXI. 33 [dp 12% 5} BROOKVILLE PINKNEY SWAN H MARBLE HILL,20 HANOVER xc uu = = oO 2 = 4 td = a x insculpta dentata,. nella jugosa 2 =a eS wea | Dinjretrorsa CLINTON, RICHMOND AND WARREN ROCKS IN INDIANA WEST OF THE CINCINNATI AN TICLINE ing Saas a ry > = Ao SP RIBRIRY oe Renae Gans NN hee OS OP aN er ate “<7 AYNIVERSITY of JELINOIS = y j ‘ . ‘ t . < . = =, é 1 = 7 ay ] > “ j , . a . THE AME PLATE XXII. an Q m 5 a Sec ee es ze = => od cee oO wa ° 2 5 g an s <= t a = bi 5 EB a uw Ca 4 Zz ea: eee Bathe SECTIONS OF CLINTON, RICHMOND, AND WARREN ROCKS IN KENTUCKY WEST OF THE CINCINNATI — ANTICLINE, BY AUG F FOERSTE. THE AMPRICAN GeoLocist, VoL. XX XI PLatsa XXII, 7 ANTICLINE, BY AUG F FOERSTE Hus owt * Elect en Se RICHMOND, AND WARREN ROCKS SECTIONS OF IN KENTUCKY WEST OF THE CINCINNATI = So = = 4 vo A COLUMNARIA ALVEOLATA B BEATRICEA UNDULATUM C CALOPCECIA CRIBRIFORMIS H COLUMNARIA HALLI L LABECHIA OHIOENSIS S STREPTELASMA RUSTICUM T TETRADIUM MINUS @Igd NIXYYM GE'SONINdS SNVOH iq 125 Feet V6E'YOCNUD 2 WITT Platystrophia Taticosta var \SO_ Feet Gelow whe Clinton W7E ‘SANOF AGHIN ZE'SIINT VS¥ TE‘ NOLONIHSYM “IW aga vaNni7vs Of HOI SADT JO 6@' ANOS SCANTS ION Ree Batti Richmond Group of Cincinnati Anticline-—Foerete. 349 section. Two feet above the base, Strophomena rugosa and Streptelasma rusticum are found. At the mouth of Bull creek, Dalmanella jugosa was not observed. Southward, as far as Raywick, in Kentucky, it is apparently absent, or at least does not form a conspicuous part of the fauna at the base of the Richmond section. The diminution in the vertical range of Dalmanella jugosa, from Hanover southward, is accompanied by a diminution in the thickness of both the Middle and Lower Richmond. In the following measurements the top of the richly fossiliferous part of the Middle Richmond has been chosen as the most easily recognized horizon near the top of the Middle Rich- mond in the southern part of the area under discussion. The thickness of the section included between the base of the Low- er Richmond and the top of the richly fossiliterous beds near the top of the Middle Richmond at Madison is 110 feet; at Hanover, 100 feet; at the Pinckney Swan locality on Saluda creek, 68 feet; at Marble Hill, 44 feet; and at the mouth of Bull creek, 30 feet. ; At the mouth of Bull creek, the Lower Richmond is only twenty feet thick. The -fossils are most numerous in the lower eleven feet, consisting of clay and a few thin beds of interbed- ded limestone. The top of the Lower Richmond is formed by a wave-marked layer of limestone. Above this are ten feet of light cdlored clay and whitish limestone, containing Dinorthis subquadrata, which form the richly fossiliferous part of the Middle Richmond. Above this somewhere should be the horizon containing massive corals. A stray specimen of Col- umnaria alveolata in a sandy matrix may have come from this horizon. A single specimen of Columnaria halli was found in the white rubble limestone forming the Middle Richmond. Il. Kentucky. The Richmond. Between the mouth of Bull creek, in Indiana, and the cross- ing of the Louisville-Bardstown pike over Floyds Fork (lo- cality 29), in Kentucky, a distance of 25 miles, the Richmond stage diminishes from 83 feet to about 66 feet; according to this, the average rate of diminution of the Richmond stage is about .7 foot per mile. Three miles south of Floyds Fork, 350 The American Geologist. gee along the creek south of Mount Washington, the thickness of the Richmond is apparently the same as at Floyds Fork, name- ly about 69 feet. However, between Mount Washington (69 feet) and the William McGrudor locality (32 feet), north of Cane spring, in the southeastern part of Bullitt county, a dis- tance of 8 miles, the average rate of diminution is about 4.6 feet per mile. The thinnest’ section of the Richmond, so far discovered in Kentucky, is located along the road leading southwest from Balltown. Here the Richmond is only 22 feet thick, indicating an average diminution in thickness, in the 13 miles south of the McGrudor locality, of about .8 foot per - mile. The Middle and Lower Richinond. The thickness of the richly fossiliferous clays and thin limestones, at the base of the Richmond stage, appears to be about the same at the crossing of the Louisville-Bardstcwn pike over Floyds Fork, and south of Mount Washington, as at the mouth of Bull creek, namely, between twenty-five and thirty feet. This suggests that the lower, richly fossiliferous part of the Richmond section at these localities includes both Lower and Middle Richmond strata. No attempt has been made as yet to distinguish between them. Strophomena ru- gosa occurs in the lower part of the Richmond section at Floyds Fork. Hebertella occidentalis has been found at the top of the richly fossiliferous section at Mount Washington. Within a distance of four or five miles southwest of Mount Washington, the very fossiliferous part at the base of the Rich- mond is reduced to about fifteen feet, and about eight miles south of Mount Washington, at the William McGrudor local- ity, in the southeastern part of Bullitt county, its thickness is only five or six feet. Farther south, in Nelson and Marion counties, the richly fossiliferous part at the base of the Rich- mond varies between six and eleven feet. It is possible that the sudden decrease in thickness of the richly fossiliferous part of the Richmond stage between Mount Washington and the William McGrudor locality is accompan- ied by the disappearance of the Lower Richmond. The evi- dence is not conclusive. Most of the fossils found in this richly fossiliferous part of the section at the William McGrudor locality, and at the numerous localities in Nel- Richmond Group of Cincinnati Anticline—Foerste. 351 son and Marion counties, belong to species gommon to both the Lower and the Middle Richmond. Among these are Hebertella sinuata, Strophomena sulcata, Rafinesquina alternata, Rhynchotrema capax, Zygospira modesta, Bys- sonychia radiata, Lophospira tropidophora, Streptelasma rus- ticum, Protarea vestusta, Tetradium minus, and various var- ieties of Platystrophia. Several species, however, are not known to have occurred earlier than during the Mfddle Rich- mond. Dinorthis subquadrata was found in the richly fossil- iferous part of the Richmond at Bardstown. -1.5'44- In a position at 90° to the first one finds 1’, > mg 1. e. Mp > 1.553. Referring to tables showing indices of refraction for various minerals, this fixes the feldspar as labradorite. In selecting minerals for comparison, the selection of feld- spar should be made with reference to a known section, such as a bisectrix. Any adjacent quartz grain may be selected, whether or not its chief axes of elasticity lie parallel with those of the feldspar grain. The value of those directions which do lie parallel to the chief axes of elasticity of the feldspar can easily be reckoned. Method for Determining feldspar and other Minerals through their double refraction by means of Michel Levy's Comparateur.* First correct the scale of the comparateur, which can not be accurately made, so that o of the scale corresponds exactly to the thickness 0 of the quartz wedge of the comparateur. Do this with the teinte sensible plate. Insert the plate in the mi- croscope below, and by shoving along the quartz wedge of the comparateur equalize successively the teintes sensibles of the first and second orders on the wedge, and read on the scale. Let these two readings be 375 and 720, symbolized by t and t’ In thin sections dispersion may be neglected. It is known that t (375 in this case) corresponds to a retardation of the light waves of 0.000575mm. and t’ (in this case 720) to one of 0.001128mm. Therefore the division of the scale taken as unit in the measurement (in above case the smallest division : II28—575 . of the vernier, symbolized by d) equals d = aa In “ef irs T128—575 millionths of millimeter. In the above case d= a 720—375 1.6087 in millionths of millimeter, or 0.0000016 millimeter re- tardation of light wave in the thickness of the quartz wedge, * MICHEL LEVY. Mineraux des Roches, p. 34, etc. 29 The American Geologist. S22 corresponding to the movement of one division of the vernier. Supposing the wedge thinned to 0, and calling this reading T128t—575t’ T120— 575) case T = 16.27; this is therefore the correction, and to be de- ducted from the readings, to obtain their actual value. A given reading on the scale may be called t’. Then e’X= (t’—T)d, when e symbolizes the thickness of the mineral and X the index of double refraction (ng—np or “—=). It is evident that to use this method directly one must know e to find X, or vice versa. The direct methods of measuring e are inaccurate, therefore in practice a method of comparison with a known e is used. In the same section with the mineral to be determined, a known mineral is selected, preferably quartz parallel to the vertical axis. It is known that in quartz X (ng — np = » — =) =.00915. The interference colors of the quartz and of the mineral to be determined are read, and cor- rected by T. Then for the mineral studied eX = A; for the A quartz eX’.= A’. From this follows X Seu or X =: T, we deduce the formula T = In the above (.00915)). If the colors are too high or too low to be distinct, use a teinte sensible quartz plate; if the colors are too low, add the teinte sensible (like axes parallel) ; if too low, subtract (like axes crossed), then add to or substract from the reading, the value of the teinte sensible on the scale, as previously determined and corrected by T. For example, the teinte sensible alone reads 370. This minus T(= 16) = 354. Ifa feldspar or other min- eral with low refraction colors is to be measured, add the teinte sensible, and read the graduation on the scale, which gradu- ation corresponds to the sum of the colors. Say e.g., this is 590: correct by T. 590—T=574. Subtract the value of the teinte sensible, 574—354—220. Above formula then becomes 220 : : bs ee Ar 00915. For too high colors subtract the teinte sen- sible. 379 ~The Determination of Feldspars.—S purr. ‘6ggr ‘sueg ‘soysoY sap xhesulyy sop xnvafqey {x1o19ey] pue Aaa y]-Jayo wiosy poydepy, .L RR te ie i nce Si | Nncn en oe wire isos wate fame oe Ach eae cee yoy pe Pe Lee wies[eg epeues 5 iS ean (Oca ees (-2) 600°0 (Oo ik ae (3) E6G+1 [oct rere eter eer eee 214eng £10°0 1100 tz0'o 6z9° I zhg' eSgr1 “*Qpua|quIOFY Use13 UOWIWIOD 300° 0 Vek oer ie $SS-1 LSS-1 FES a aysouy £00°0 S00°0 g00'O vSS"1 LSS oT ZS te? OAs aha eee eae apiopeiqe’y] ooo £00°0 Z00°0 6bS "1 Gooer OES Ces eae) matte ee ouIsapuy Foo0°o -¥oo'o g00°0 peSer ges 1 evs *I gee Seep ee ct OSE ser eae 900'0 3000 zesey peS'r Fe en RE Cer heer a Ee anqry go0o0'o 100°0 £00°0 €cS "1 62S" OSGaT Ae hal ae tree se ‘asRepIOyWOUYy £00°0 £00°0 £00°0 0} 900°0 coat gzS I OS Sra al ee ae ee see ES SUIPIOITY S00°o z00*0 £00°0 61S 1 2S "1 DE Cine, Mane Wary aps eee et asepDOyUO u 3 \ ee i eS oe eas } (oi Vico Gear ar] (Fn) (22) A} (di) ” soxv |S SS . _0}‘daad auvid | 0} ‘dad aueta o143d0 jo auRid STVYANIWN " yYSIT MOl]IA) SNOROeS ‘NOILOVUAAY AO SHOIGN] IVdIONINdG TVdIONIUYU AO NOILOVYAAY ATAHNOC x 9PUI|qUIOFY U9aIDH UOMTOD pure zen’) YM ‘saI90ds sedsppay JOJ UOIDRAJOY VTQnOG, pur I[SuIG Jo s[qvy, 380 The American Geologist. Te ae Methods for Determining Feldspars by Ascertaining the Position of the Optic Axes. These methods are among the most practical and accurate. It is well known that in feldspars the position of the optic axes varies regularly in regard to the crystallographic boundaries according to the change of chemical composition, and it is only necessary, therefore, to define the relation of the axes to these boundaries to determine the feldspar. 3 Michel Levys Method.—This method, with more or less variation, has been lately much used in this country. In its original form, as proposed by the great French mineralogist, it may be described briefly as follows: For this method feldspars must be twinned. If twinned after the albite law, find a section in the zone of symmetry, or nearly so. This zone is characterized by having the extinction angle in the two individuals on both sides of the twinning plane the same. If the angle of the position of equal illumination of the two individuals with the twinning line is greater than that of the position of extinction with the same line, the feld- spar is more acid than oligoclase; if more basic, the reverse. If the feldspar is twinned after both albite and Carlsbad laws, discover this by bringing the alhite lamellz in position of equal illumination—then the Carlsbad twinning will still show its differences of extinction. Find such a crystal in the zone of symmetry or nearly so, by the above method. Read the extinction angle on one side of the Carlsbad twinning plane and then on the other. Suppose these are 38° and 21°. Refer to Michel Levy’s plates.* The vertical red line is the projection of the zone of symmetry. On the upper half of the projection the red figures equal + angles of extinction on the zone of symmetry ; on the lower half the black ones equal — angles on the same zone. In Carlsbad twinning the two individuals are turned on vertical twinning axes 180°. so that the negative parts of one individual become side by side with the positive parts of another. Therefore, the two angles read on the two sides of the twinning plane correspond to the positive and the negative readings. They must be sought on the upper half and * A thorough article on this subject, with reproductions of the diagrams of Michel Levy has been published by PROFESSOK N. H. WINCHELL, this journal, wo]! xxi; No. a". The Determination of Feldspars,—S purr. 381 the lower half respectively of the vertical line which is the pro- jection of the zone of symmetry. In ordinary sections, it is impossible to determine which reading is positive and which negative, but the two readings are conjugated with respect to the center of the projections—that is, appear at equal dis- tances from the center. Therefore the projection is sought out in which the two readings have the necessary conjugation —in the above case the figures point to labradorite Ab, An,. If a section is not cut exactly in the zone of symmetry, the angles on each side of the albite twinning line will vary, and their values will be at equal distances to the right and left of the vertical line, the distance varying with the deviation from the zone of symmetry. Fouque Method—Find a bisectrix in convergent light and determine its optical character. To do this first bring the section into the position of extinction, when a cross is formed. Next, rotate the stage 45°, noticing the direction in which the hyperbole move out of the field, and bring the line joining the apices of the curves into the 45° position in diag- onally opposite quadrants of the field. In this position deter- mine by means of the quartz wedge, teinte sensible, or gypsum plate, whether this line is of greater or less elasticity than the bisectrix perpendicular to which the section is cut. The quartz wedge is ordinarily the most convenient means, and in using it remember that when like axes are superposed the colors of the section rise, and that when they are crossed the colors fall. _Tf the line joining the hyperbole, which lies in the plane of the optic axes, is the direction of greatest elasticity in the section (a.) then the section is cut perpendicular to a positive bisec- trix. If this direction is that of least elasticity (c) the bisec- trix is negative. Now bring the trace of the optic axes into position parallel with one of the cross-hairs and measure the angles by the method stated below. It is often convenient to remember that the positive bisectrix always emerges upon the brachypinacoid. If the bisectrix is positive, measure the angle between it and the trace of the basal plane. This may be re- cognized in the section as a crystal boundary or as a cleavage. If these are not present the angle may be measured against the pericline twinning planes, but in this case it is necessary to remember that this twinning plane is usually not exactly *‘soooid aSeawad UO a[qBurursdjz2q + “*QS[OIA 1OF PVG} UBY} SS2J St pat 103 [Suv o13do ey} SurAyusig , 3 S eo orouer ms Lezs'1 5b OF o£ 4060 fess _|ersscssess]escenssnvecestecsaee|ecsssoneas oaeesseess] o2eee+- 9B BIIOUZIC g oAG + | oAGI+ | 9E9'T oOL o88 A<¢?| — o88 ol8 G's9 j09S*S J" aULPIOATI] 2 o6 + 0G + 8eC'L ob 0& 088 hae? a 009 o8h 89 |0L9°% eae UTPIOIII YP, Ae) op 0G + 8ec'T SOr OE 088 Nee Sra oSY o8L 89 |O8G ¢ | eSB]S0lI10uy 5 oAGI+ Gre ats PEST 0€ o6T oF A<¢ aie oLL o8L BO. |OLOIG |S 7 S55 So TQ, 3 oAOL+ | oAG + oFS'T o0& OT 0€ oF8 RESO + |.%”88 oL8 G9 |OP9'?S | OFIqITB Nya , ; -ISBJIOS1|0, = 68 | a6 + Peers yt of . 88 / Np UE |e et to ofL =. | FO [SFOS | asB]PO31O S Opel ee esc'T oS oGL A oSG— olI— | S9S'T o$& 0O& 08S Ko TO eae oLL | O€ 6h | FS jSOL'S |" "AMUMO7z4hq Ss ; “1OpBsqe’y Ea etl y—-| >A9e— esol oOF oLG Ne) NOLL oSé Pr Soli] | eu Mo yg ny oAL¥— | oAIE— ose l o8P OG 09S A > od Sele, oG& A me hf eat (ea o4s1qqziouy = ww - ae ne =: I t OtO BES Ay $a 58 =e eae ENe au} Bes dere pv 0 09 > 5208 S| +2 & 509 jO W0}}0a8SI9}U1 JayzjoUOIDass9ju1| TSoka | & = 3 &8 8 S 5 G@eSncalForadnl 4 & ay} JO 2033 ay} | 242 j0 9vIVA47 | ZaSBE | Ss pda ho alert pete )a7 oe or el meres Oa oClmnaaag| Ps puv saxv ondo | puvsaxvoyjdo |eRGen | as | gah | ¢e@ar5 | 2 | a O ‘AVdSd Tad Beate | ta eter] Ps 243 jo aud ay} | eqzjyoouvjdany | aes os] oe pA, ones | ge a) O oo8ogx Stpoge Bs = |yo 99813 a4} u9AM}|j0 998.17 94} UD9AM}| KABES 2 8 as | ese a Ee [plate es A Rooteciote8 ha) § 8 [aq ‘x1jz008iq aay] aq ‘x1az00sIq aay] -R ES Bo | ae | Gag eo | se | SP Sato Has 35958 Bee Oes 30 -isod ay} 0} 48] | -eSau aq}, 034", |F REGS | oS Guitis| Beene yal ecs|| or : On met ye a OS al -noipuadsad uo | -noipusdiad u01n | BFE Se | Ga RM) tat sao RN Bao Srorto -238 94} ud a|Sue | -oas ay} UOajSuv]* ® BR] oe te) hy 2 a po tg Oda sla melodie =) U01}00I}x29 2Yy | uOol1ZOUI xd au. (e,4) ie ‘ANGAOY OL DNIGHODDY SuVdSdTaA, AHL JO NOILLVNIWUYALAG The Determination of Feldspars.—S purr. 383 parallel to the base, but varies from it according to the differ- ent species, by an angle which must be added or subtracted from the reading, according to the case, to get the true angle with the base. If the bisectrix is negative, determine the angle between the trace of the optic plane and that of the brachypinacoid, The latter may be represented in a section either by a crystal edge, by a brachypinacoidal cleavage or by twinning planes of the albite or Carlsbad laws. . In either case find the angles corresponding to the species in the accompanying tables. REVIEW OF RECENT GEOLOGICAL LITERATURE. State Geolegical Survey of North Dakota, Second Biennial Report. Frank A. Wiper, State Geologist. Pages 262; with 39 plates, 21 figures in the text, and two folded maps. Bismarck, December, 1902. This survey was begun in the year 1899, under the direction of pro- fessor E. J. Babcock, professor of chemistry and dean of the College of Mines in: the University of North Dakota, at Grand Forks, with a very small appropriation from the state. His report on the general topographic and geologic features of the state, and on its clays of eco- nomic value, lignite, and water resotirces, in 103 pages, was the first biennial report of this survey, published in the early part of 1901. With the appointment of Mr. Wilder as professor of geology in the univer- sity, the direction of the state survey was transferred to him; and, in co-operation with the U. S. Geological Survey, he has been enabled to enlarge the scope of this work. About two-thirds of this report are descriptions and discussions of the valuable lignite coal deposits which occupy the western half of the state, with the Turtle mountains as.an outlying area farther east. Pro- fessor Wilder was assisted by Mr. L. H. Wood in this part of his work. The lignite beds, in their workable development, are restricted to the Laramie series of clays and sandstones; and the seams of lignite vary in thickness from an inch to forty feet. Many seams are often found in the same vertical section, and some of them are traced five or six miles, or more, as in the bluffs of the Little Missouri river; but gener- ally they vary greatly in thickness within such distances, and frequenitly are of much less extent, thinning out entirely, and giving place to new seams a little higher or lower. Along the Northern Pacific railway in the region of Dickinson, Medora, and Sentinel Butte, and thence for 384 The American Geologist. ras 4 forty or fifty miles southward, lignite beds fifteen feet thick are not un- commion, and some extensive seams are twenty-five feet thick. During the year 1902 the output of North Dakota lignite coal was 296,800 tons, with a value, at the mines, of $407,000, being more than twice the amount and value of its production in the year Igoo. Professor Babcock contributes as the final part of this report, an im- portant paper of forty-three pages, on the “Water Resources of the Devil’s Lake Region.” It is found that this lake during the last twenty years has ranged from four to nine feet lower than it was in 1883; and its ancient high shore lines are twenty to thirty feet above the present water level. The greatest depth of water now found by soundings, in the central part of the main lake, is twenty-nine feet. Thus the alkaline Devil’s lake, so called in translation of its Sioux name, probably alluding to the bitterness of its water, which is the largest lake of North Dakota, about thirty-two miles long, with a very irregular area, has now no more than a sixth or an eighth so much volume as immediately after the retreat of the ice-sheet from this area, when, as an enlarged expanse of fresh water, it reached east into the basin of Stump lake, and thence outflowed southward to the Sheyenne river. W.. U. The Cause of the Glacial Period, being a Resume and Discussion of the Current Theories to account for the Phenomena of the Drift, with a New Theory by the Author. By H. L. True, M.D., Member of the Ohio State Academy of Science. Pages xi, 162; with 7 plates, and 9 figures in the text. Cincinnati. The Robert Clarke Co., De- cember, 1902. The various theories which attribute continental glaciation to chang- es in the astronomic relations of the earth, as advocated by Croll, Ball, Drayson, Becker, and others, are reviewed and discarded by Dr. True; and the usual theories appealing to geographic changes, as great ele- vation of the lands that became enveloped by snow and ice, held by Lyell, Dana, LeConte, Upham, Very, Wallace, Wright, and others, are also considered insufficient or improbable. Variations in the amount of heat received from the sun, or in its retention by the earth’s atmosphere, with changes in the proportions of water vapor and of carbon dioxide in the air, as recently proposed by Arrhenius and Chamberlin to account for the Glacial period, are also thought to be inapplicable to this problem. : Instead of all these rejected hypotheses, Dr. True advances one original with himself; which, however, agrees with the view presented by Upham, in an appendix of Wright’s “Ice Age in North America,” by associating the glaciation of continental areas with the very extra- ordinary crumpling of the earth’s crust and upheavals of mountain ranges which have characterized Late Tertiary and Quaternary time. The new theory is stated as follows: “Up to and during the princi- pal part of the Tertiary period the earth had so far cooled and the rocky crust had become so thickened that it sustained the pressure of Review of Recent Geological Literature. 385 the arch for a long time, but finally the point was reached when it could sustain it no longer. ‘The last grain of sand broke the camel’s back.’ The arch gave way or crumpled into the form of mountains, and as the crust was thicker at this time than any time previous, so were the upheavals in the form of mountains greater than any that had preceded them, and of course the troughs formed from the settling of the arch would be greater; thus the beds of the oceans settled down, forming deeper basins, thereby draining the polar regions and leaving them above water (especially was this the case around the North Pole), depriving them of their warm ocean currents, or water covering, and allowing them to cool off and begin to form ice caps. The warm cli- mate of the Tertiary period continued until the settling process had so far drained the polar regions as to allow ice.to begin to form when the climate began to change, which change continued until the Tertiary merged into the Quaternary. Thus began the formation of ice which finally culminated in a Glacial period. The conditions present were these: A land foundation around the poles for ice to rest upon. The circulation of the ocean shut off or confined to the regions south of the land barrier, but having free circulation within the tropical regions. The ocean thus confined would become warmer than it had previously been. If it had been carrying a certain amount of heat to. be dissipated around the poles, and on account of the land barriers this heat were to be confined south of the polar regions, what would prevent the water from becoming warmer? Here we have a steaming ocean to furnish the vapor and a cold land surface to precipitate the snow, , the condi- tions in perfection to produce a glacial period.” Dr. True proceeds further, to account for the geologically sudden and recent close of the Ice age, so far as it affected the now temperate latitudes, by introducing another grand cataclysm during the Cham- plain epoch. Here he supposes, as was suggested in 1866 by Sir John Evans, that, while the earth’s axis probably remained unchanged in its direction, a comparatively thin crust of the earth may have slipped as a whole upon the much larger nucleal mass so that the locations of the poles upon, the crust have been changed. “North America and western Europe,” says Dr. True, “moved down out of the cold region, while northern Siberia, on,.the opposite side of the earth, moved up into it. A slight and imperceptible move- ment in this direction had, no doubt, been goimg on for ages, as the load accumulated on one side of the earth, but at the time of which I am speaking something broke loose and precipitated a rush. A cataclysm was produced that submerged the North Atlantic region and southern part of the United States, and carried the earth beyond the point of equilibrium. Of course, the balance was finally established by the waters of the ocean, which, being free to move, rushed upon the land in the form of great tidal waves, which surged back and forth for a time, but finally settled down to a state of tranquility, while the diurnal revolutions of the earth went grandly on upon the old axis, with per- haps a slight break or variation from its usual regularity. 386 The American Geologist. June, 1903. It is not probable that either geologists or physicists will approve this theory, which is a contribution by a layman to the already !arge number of attempts to explain the wonderful climatic changes causing and ending the Ice age. Like the carbon dioxide theory, it has a some- what near relationship with the more simple explanation that has been advocated by the present reviewer, namely, elevation of continental areas as high plateaus above the snow line, and, when they became heavily loaded with ice-sheets, their depression beneath that weight, accounting for the Champlain epoch and the end of the Glacial period, excepting in the Arctic and Antarctic regions. w. U. Existence du Cretace inferieur en Argolide Grece—Existence du Jur- assique sup. et de l’infracretace dans lVisle de Crete—etc., etc., par L. Cayrux [Comples Rendus de l’Academie des Sciences, Paris, 1903]. These are preliminary notes on observations made in Greece and the island of Crete on the Mesozoic rocks appearing in that part of the Mediterranean. The structure of the terranes in its overturned group is compared with that of the southern Tyrol. An interesting discovery is that of a radiolarian ooze in the Argolid which he thinks has affinities with radiolarians of the Neocomian in the Tyrol. In Crete the composition of the beds is very varied, running from fine-grained calcareous sandstones to coralline limestones, clays, schist and jaspery beds; the fragmentary rocks take on the appearance of flysch. Several localities for fossils were found, brachiopods and corals predominating; there are also sea-urchins. : One note is given to a description of the rocks connected with vol- canic eruptions of the Mesozoic time. Intrusive rocks predominate, and are both basic and acid. The author remarks that the “eruptive rocks metamorphosed the upper terranes among which they are in- cluded, and have left absolutely intact, the more recent terranes on which they repose” [as effusives]. He further remarks that the great quaternary subsidences of the Egean sea and this concomitant only represent the last episodes of the phenomena, the first manifestations of which go back to Jurassic times. GF. M. MONTHLY AUTHOR’S CATALOGUE OF AMERICAN GEOLOGICAL LITERATURE ARRANGED ALPHABETICALLY, ADAMS, GEO. I. Zine and lead deposits of northern Arkansas. (U. 8S. G. S. Bull. No. 213, Ser. A, 1902, pp. 187-197.) ALDEN. WM. C. The stone industry in the vicinity of Chicago, Ill. (U. S. G. S. Bull. No. 218, Ser. A, 1902, pp. 357-361.) Authors Catalogue. 387 ASHLEY, GEO. H. (and M. L. FULLER). Recent work in the coal field of Indiana and Illinois. (U.S. G.S. Bull. No. 2138, Ser. A, 1302, pp. 284-294.) BOUTWELL, J. M. Ore deposits of Bingham, Utah. (U.S. G.S. Bull. No. 213, Ser. A, 1902, pp. 105-123.) : BOUTWELL, J. M. Progress Report on the Park Cily Mining District, Utah. (U.S. G. S. Bull. No. 213, Ser. A’, 1902, pp. 31-41.) BROOKS, A. H. Placer Gold Mining in Alaska in 1902. (U. S. G. S. Bull. No. 213, Ser. A, pp. 41-49.) BROOKS, A. H. Stream tin in Alaska. (U. S. G. S. Bull. No. 218, Ser. A, 1902, pp. 92-94.) CAMPBELL, M. R. Basin-Range Structure in the Death Valley region of southeast- ern California. (Am. Geol., vol. 31, May, 1993, p. 311.) CAMPBELL, M. R. Borax deposits of eastern California. (U.S. G. S. Bull. No. 213, Ser. A, 1902, pp. 401-406.) CAMPBELL, M. R. Recent work in the bituminous coal fields, Pennsylvania. GULLS: G. S. Bull. No. 213, Ser. A, 1902, pp. 270-276.) CLARKE, F. W. Pseudo-Serpentine from Stevens Co., Washington. (Am. Jour. Sei., vol. 15, May, 1903, pp. 397-399.) GOLLIER;, A. J. . Coal resources of the Yukon Basin, Alaska. (U. S. G. S. Bull. No. 213, Ser. A. 1902. pv. 276-284.) COLLIER, A. J. The Glenn Creek Gold Mining District, Alaska. (U.S. G. S. Bull. _No. 213, Ser. A, 1902, pp. 49-57.) DALE, T. NELSON. The slate industry of Slatington, Pa., and Martinburg, W. Va. (iees..G. .S: Bull. No. 213, Ser. A,-1902, pp. 361-365.) DICKSON, CHAS. W. Note on the condition of Platinum in the Nickel-Copper ores from Sudbury. (Am. Jour. Sci., vol. 15, Feb., 1903, pp. 136-140.) DICKINSON, H. T. Quarries of Bluestone and other Sandstones in the Upper Devon- ian of New York State. (Bull. 61, N. Y. State Mus., pp. 104, 1903.) DILLER, J. S. Klamath Mountain Section. (Am. Jour. Sci., vol. 15, pp. 342-363. May, 1903.) 388 The American Geologist. Same, MaGee DILLER, J. S. Copper deposits of the Redding district, California. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 123-133.) DIEEEIR Jas. Limestone of the Redding district, Cal. .(U. S. G. S. Bull. No. 218, Ser. A, 1902, p. 365.) DILLER, J. S. Iron ores of the Redding quadrangle, California. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 219-221.) DURYEE, EDW. Cement investigations in Arizona. (U.S. G. S. Bull. No. 213, Ser. A, 1902, pp. 372-381.) ECKEE,.E: C. Utilization of iron and steel slags. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 221-232.) ECKEL, E. CG. (and C. W. HAYES:) Iron ores of the Carterville district, Georgia. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 233-248.) ECKEE EAC: Stoneware and brick clays of western Tennessee and N. W. Miss. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 382-392.) ECKEE RE: GC: Salt and gypsum deposits of S. W. Virginia. (U.S. G. S. Bull No. 213, Ser. A, 1902, 406-417.) EGKER EG: The white phosphates of Decatur Co., Tenn. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 424-426.) ECKEL, E. C. (and C. W. HAYES.) Occurrence and development of ocher deposits in the Cartersville district, Georgia. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 427- 433.) ECKEE E.G: Gold and Pyrite deposits, Dahlonega district, Georgia. (U.S. G. S. Bull. No. 213, Ser. A, 1902, pp. 57-64.) ELDRIDGE, GEO. H. Origin and distribution of asphalt and bituminous rock deposits in the United States. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 296-306.) ELDRIDGE, GEO. H. The petroleum fields of California. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 306-322. EMMONS, S. F. Platinum in copper ores in Wyoming. (U.S. G. S. Bull. No. 213, Ser. A, 1902, pp. 94-98. EMMONS, S. F. (and C. W. HAYES). Contributions to Economic Geology, 1902. (U. S. G. S. Bull. No. 213, Ser. A, Economic Geol. 24.) Author's Catalogue. 389 FENNEMAN, N. M. 2 The Boulder, Colo., oil field. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 322-333.) FINLEY, GEO. lI. The Granite Area of Barre, Vt. Rep. of the Vermont State Ge- ologist, pp. 59, 1902.) FULLER, M. L. : Asphalt, oil and gas in S. W. Indiana. (U.S. G.S. Bull. No. 213, Ser. A, 1902, pp. 333-336.) FULLER, M. L. (and GEO. H. ASHLEY.) Recent work in the coal field of Indiana and Illinois. (U.S. G.S. Bull. No. 2138, Ser. A, 1902, pp. 284-294.) GERDINE, T. G. (and D. C. WITHERSPOON.) Explorations among the Wrangall Mountains in Alaska. (Nat. Geographic Mag., vol. 14, No. 4, April, 19038, p. 161.) GRABAU, A. W. Studies in Gastropoda. (Am. Nat., vol. 36, No. 432, pp. 917-345, Dec., 1902.) GRISWOLD, W. T. Structural work in 1901 and 1902 in the eastern Ohio oil fields. CU. Ss) Gals.) Bull No: 213; Ser. “A, pp. 3386-345.) HARRINGTON, B. J. Composition of some Canadian Amphiboles. (Am. Jour. Sci., vol. 15, May, 1903, pp. 392-395.) HAYES, C. W. Manganese ores of the Cartersville district, Georgia. (U. S. G. S. Bull. No. 2138, Ser. A, 1902, pp. 233-243.) HAYES, C. W. Coal fields of the United States. (U.S. G. S. Bull. No. 213, Ser. A, 1902, pp. 257-270.) HAYES, C. W. Oil fields of the Texas-Louisiana Gulf coastal plain. (U. S. G. S. Bull., No. 218, Ser. A, 1902, pp. 345-353.) HAYES, C. W. Asphalt deposits, Pike county, Ark. (U. S. G. S. Bull. No. 218. Ser. A, 1902, pp. 353-356.) HAYES, C. W. Origin and extent of the Tennessee white phosphates. (U.S. G. S. Bull. No. 2138, Ser. A, 1902, pp. 418-424.) HAYES, C. W. (and S. F. EMMONS.) Contributions to Economic Geology. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 450.) HILGARD, E. W. Subterranean Water Supply of the San Bernardine Valley. (U.S. Dept. Agr., Report of Irrigation Investigations, pp. 103-145, 1901.) 390 The American Geologist. SU ee HOBBS, W. H. Tungsten Mining at Trumbull, Conn. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 98-99.) KEITH, ARTHUR. Iron ore deposits, Cranberry district, N. Carolina—Tennessee. (U. S. G. S. Bull. No. 2138, Ser. A, pp. 248-247.) KEITH, ARTHUR. Tennessee Marbles. (U. S. G. S. Bull. No. 213, Ser. A, pp. 366- ciate) KEITH, ARTHUR. Talc deposits of North Carolina. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 433-439.) KEMP, J. F. Igneous Rocks and circulating waters as factors in ore deposition. (Trans. Am. Inst. Inst. Min. Eng., Oct., 1902, pp. 16.) KUMMEL, H. P. Glacial Geology of New Jersey (Salisbury), vol. 5, Final Report of the State Geologist, pp. 802, pls. 66, Trenton, 1902. EEE VOW. oie The Canyons of Northeastern New Mexico. (Jour. Geography, Vole t2) INOl2; seb wl 903eoppseaize LEITH, C. K. : Geologic work in the Lake Superior iron district during 1902. (U. S..G. S. Bull. No. 2138, Ser. A, 1902, pp. 247-251.) LINDGREN, WALDEMAR. Neocene rivers of the Sierra Nevada. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 64-66.) LINDGREN, WALDEMAR. Mineral deposits of the Bitterroot Range and the Clearwater Mountains, Montana. -(U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 66-71.) LINDGREN, WALDEMAR. Copper deposits .at Clifton, Arizona. (U. S. G. S. Bull. No. 2138, Ser. A, 1902, 133-141.) MENDENHALL, W. C. (and F. C. SCHRADER.) Copper deposits of the Mount Wrangell region, Alaska. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 141-149.) MENDENHALL, W. C. The Chistochina gold field, Alaska. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 71-76.) RANSOME, F. L. Copper deposits of Bisbee, Arizona. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 149-158.) ROGERS, AUSTIN F. Some new American species of Cyclus from the Coal Measures. (Contributions from the Geol. Dept., Col. Univ., vol. 10, No. 88.) SALISBURY, R. D. The Glacial Geology of New Jersey, vol. 5, Final Report of the State Geologist, pp. 802, pls. 66, Trenton, 1902. Authors Catalogue. 391 SCHRADBER, F. C. (and W. C. MENDENHALL). Copper deposits of the Mt. Wrangell region, Alaska. (U.S. G. S. Bull. No. 213, Ser. A, 1902, pp. 141-149.) 5 SCHIMER, H. W. Petrographic Description of the Dikes of Grand Isle, Vt. (Rep. State Geologist of Vermont, 1902, pp. 173-183.) SMITH, W. S. TANGIER (and E. O. ULRICH). Lead, zinc, and fluorspar deposits of western Kentucky. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 205-214.) SMITH, W. S. TANGIER. Lead and zinc deposits, Joplin district, Missouri-Kansas. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 197-205.) SMITH, GEO. OTIS. . Gold mining in central Washington. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 76-81.) SPENCER, A. C. Manganese deposits of Santiago, Cuba. (U.S. G. S. Bull. No. 2138, Ser. A, 1902, pp. 251-256.) SPENCER, A. C. Mineral resources of the Encampment copper region, Wyoming. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 158-163.) SPENCER, A. C. Reconnaissance examination copper deposits at Pearl, Colo. (U. Ss. G. S. Bull. No. 2138, Ser. A, 1902, pp. 163-170.) SPURR, J. EDW. Ore deposits of Tonopah and neighboring districts, Nevada. (U. Ss. G. S. Bull. No. 2138, Ser. A, 1902, pp. 81-88.) ULRICH, E. O. (and W. S. TANGIER SMITH). Lead, zinc, and fluorspar deposits of western Kentucky. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 205-214.) VAUGHAN, T. WAYLAND. Fuller’s earth deposits of Florida and Georgia. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 392-400.) WARD, H. A: The Andover Meteorite. (Am. Jour. Sci., Vol. 15, Mar., 1903, pp. 395-397.) WEED, W. H. Gold mines of the Marysville district, Montana. (U.S. G. S. Bull. No. 213, Ser. A, 1902, pp. 88-90.) WEED, W. H. Tin deposits of El Paso, Texas. (U. S. G. S. Bull. No. 213, Ser. A, 1902, pp. 99-103.) WEED, W. H. Ore deposits at Butte, Montana. (U.S. G. S. Bull. No. 213, Ser. A, 1902, pp. 170-181.) WEED, W. H. Copper deposits of the Appalachian States. (U.S. G. S. Bull. No. 218, Ser. A, 1902, pp. 181-186.) 392 The American Geologist. cherie WEEKS, F. B. Tungsten ore in eastern Nevada. (U.S. G. S. Bull. No. 213, Ser. AS 1902) sp: 208.) WHITEAVES, J. F. Description of a New Species of Matheria from the Trenton Limestone at Ottawa. (Ottawa Naturalist, vol. 17, Apr., 1903.) WINCHELL, H. V. Amorphous Precipitates. (Eng. and Min. Jour., Vol. 75, No. 18, May, 19038, p. 661.) WINCHELL, N. H. The Pleistocene Geology of the Concannon Farm near Lansing, Kan. (Am. Geol., Vol. 31, May, 1903, pp. 263-309.) WINCHELL, ALEXANDER N. Note on Titaniferous Pyroxene. (Am. Geol., Vol. 31, May, 1903, pp. 309-311.) WITHERSPOON, D. C. (and T. G. GERDINE). : Explorations among the Wrangall Mountains in Alaska. (Nat. Geographic Mag., vol. 14, No. 4, April, 1903, p. 161.) ; WOLFE; J. E. Zine and manganese deposits of Franklin Furnace, N. J. (U.S. G. S. Bull. No. 213, Ser. A, 1902, pp. 214-218.) WORTMAN, J. L. Studies of Eocene Mammalia in the Marsh Collections. (Ami Jour. Sci., Vol. 15, May, 19038, pp. 399-414.) CORRESPONDENCE. Tue Rock Name ANortHosytTEe. By professor Cushing made aware of his article in THe American Geoxocist, March, 1902, where also my name is mentioned, I should like to explain my views in regard to the term anorthosyte. Cushing says, that the only objection urged against the name which has come under his notice and which seems to him to be valid, has been urged by me (Die Labradorfelse des westlichen Norwegens, 1). I there argue that the name is equally applicable to an albite or oligo- clase rock, and that these are too acid,to be grouped with rocks, which are properly regarded as end series of the gabbro family. As such rocks are of the rarest kind, I agree, that my objection has most theoretical interest, but it has nevertheless its value. In the Ekersund area, where I have examined the rocks exactly, I have described the special rocks under the names labradorite rocks and bytownite rocks, and it is still my opinion, that where the rocks have been exactly examined, it is best to apply these conciser names. In the Ekersund area most of the rocks were labradorite rocks, and therefore - Correspondence. 393 the whole area has been described by me as a labradorite rock area, the same name as the earlier geologists have used. For the purpose of mapping I agree with the American geologists, that it would be necessary to have a group name. And where it is desirable to have a group name, I cannot find that we have any better than anorthosyte, which long ago has been used by the Canadian geol- ogists. And if I have proposed no substitute, it is because, I thought, that in spite of the objection above mentioned it might be desirable to have a practical group name, and then anorthosyte was the most fitting. To replace anorthosyte with plagioclasyte 1s not necessary. We should then have two names for the same rocks, and I think the petrographical nomenclature is rich enough before. For my part I cannot use the name anorthosyte as title of my new ’ paper “Die Labradorfelse des westlichen Norwegens II,” but in the text I have called attention to the fact that these rocks might be called anorthosytes, because they consist both of labradorite rocks and and- esine rocks. I have also used the name anorthosyte in my lectures because my studies of the plagioclase rocks in the areas of Ekersund, Bergen and Loften have shown that oligoclase, andesine and bytown- ite rocks occur, together with the labradorite rocks. These studies have also convinced me, that the term anorthosyte has its value in the petrographical systematism as a group name for the leucocrate links of the gabbro and dioryte families correspondent to the pyroxenytes and other melanocrate rocks. And as we on a more exact examination divide the pyroxenytes in diallagytes, etc., we also have to divide the anorthosytes in oligoclase rocks, andesine rocks, etc. The chemical and petrographical character of the different subdi- visions of the anorthosytes is rather’well known. The albite and an- orthite rocks are very rare, and I have not seen any analysis of them. The chemical relation between the other subdivisions can be seen by. the following analyses, especially of Norwegian rocks, which I know from my own examinations. li, II. ge IV SiOe. 64.98 57.34 53.42 ; 4725 AleOz. 19.50 25032 28. 36 31.56 FeoO3. PATS 1.10 1.80 men FeO .. 0.30 0.94 ai et Be 2G MgO 0.50 0.25 0.31 On27 CaO 3.70 7.99 10.49 15.30 Na2O 6.09 5.37 4.82 2.52 KO. 2.01 ea 0.84 0.37 I. Oligoclase rock. Ostvaagé, Lofoten. (Kolderup: Lofotens og Vesteraalens gabbrobergarter. Mit einem Resumé in deut- scher Sprache. Bergens Museums Narbog 1808). II. Andesine rock. Fosse, Bergen. Will be published in my new paper. Die Labradorfelse des westlichen Norwegens II. Ill. Labradorite rock. Ogne, Ekersund. (Kolderup: Die Labra- dorfelse des westlichen Norwegens. Bergens Museums Nar- bog. 1896). IV. Bytownite rock. Beaver bay, Minnesota. (R. Irving: Copper- Bearing Rocks of Minnesota). CARL FRED KOLDERUP. 394 The American Geologist. June, eles PERSONAL AND SCIENTIFIC NEWS. PROFESSOR T. C. CHAMBERLIN delivered a lecture on “The nebular hypothesis” at Northwestern University on April 29th. Horace V. WINCHELL will examine, the coming summer, the reputed copper districts of Alaska, entering the country by way of Valdes. Proressor Russert D. GrorGe, of the State University of Iowa, has accepted the professorship of geology in the State University of Colorado. Dr. C. P. Berkey, assistant professor of geology and min- eralogy at the State University of Minnesota, has accepted an appointment to a similar position in Columbia University, New York, beginning in September. Proressor N. H. WiNcHELL is making geological eco- nomic explorations in the vicinity of Flathead lake, Montana, and is likely to be absent from Minneapolis the greater part of the summer. Mr. Ernest F. BurcHARD, at present teaching chemistry and geology in the Sioux City high school, has been appointed to a fellowship in geology at Northwestern University, from which institution he obtained his bachelor’s degree three years ago. ALBERT HUNTINGTON CHESTER, curator of the geological museum and professor of chemistry and mineralogy at Rut- gers College, New Brunswick, N. J., died on April 13 from pneumonia. He was a graduate of Union College, and at one time taught at Hamilton. GEOLOGICAL EXCURSION TO DEVILS LAKE AND THE DALLES OF THE WisconsiIN. On April 16th, 17th and 18th Professor C. R. Van Hise conducted a party of about seventy-five stu- dents from the University of Wisconsin and from Northwestern University to these localities. Mr. Baitey Writs has accepted the position of leader of the Carnegie Geological Expedition to China, which has as its object the investigation of the Cambrian of that country. He will be assisted by Mr. Eliot Blackwelder of the University of Chicago. Mr. Willis expects to leave Washington in July, to attend the International Congress of Geologists at Vienna, and to go to China via Siberia. Dr. H. Fosrer Batn has accepted an appointment as geolo- gist on the United States Geological Survey, and during Mr. Bailey Willis’s absence in China ‘Dr. Bain will be acting ‘editor of geologic folios. He is to take up the study of the lead and poh, Personal and Scientific News. 395) zinc deposits of the Mississippi valley, and during the coming summer will make special investigations concerning these de- posits in southern and northwestern Illinois. PROPOSED TOPOGRAPHICAL MAP OF MicHIGAN. The late meeting of the Michigan Academy of Science took action look- ing to the completion of the topographical map of Michigan. In his presidential address professor I. C. Russell reviewed the subject and suggested united effort. The state survey is to co-operate with the United States Geological Survey. In addition to present funds available the state is asked to appro- priate $1000 per year. At THE New Mexico ScHoor or Mines the work of min- ing engineering will be specialized along three distinct lines. These are the mechanical, the metallurgical and the geological. The last mentioned will form a somewhat new departure in this country and will be known as the special course in Geology of Mineral Deposits. It will be under the direct supervision of president Keyes. There will be four instructors in the geolog- ical department of this institution. In tHE NEw Mexico ScHoot or MINEs, six new profes- sorships have lately been provided for. These chairs will be filled during the summer. The departments thus established are Mineralogy and Petrography, Mining, Mechanical Engin- eering, | Metallurgy, Physics and Electrical Engineering, and Languages. Several special lectureships and associate pro- fessorships have also been established. Particular emphasis is placed on the lectureship and study of Mining Law. THE MOST IMPORTANT PROBLEM in the manufacture of the peat into a commercial article is the economical removal of the moisture. This is now done by drying. After this process the peat is pressed into small bricks. The manufactured product must be kept dry, otherwise it becomes valueless for heating purposes. The cost of manufacture is from $1.50 to $2.00 a ton, and the cost of selling about the same. This means that the product will sell for from $3 to $4 a ton, and must find market in competition with anthracite coal. GEOLOGICAL EXCURSION TO THE LAKE SUPERIOR DISTRICT. Professor C. K. Leith, of the University of Wisconsin, con- ducted a party of students and geologists to the Vermilion, Mesabi, Gogebic and Marquette iron ranges and also to the copper region of Keweenaw point for a ten days’ excursion ( April 20th to 28th). There were present fifteen students from the University of Wisconsin, one from Northwestern Univer- sity and one from the University of Chicago; also the follow- ing geologists: F. D. Adams, A. E. Barlow, J. M. Clements, UPS: “Grant, We JH. ‘Hobbs, C. K. Leth; A. P. Low, A. E. Seaman, C. E. Wright and F. E. Wright; also Kirby Thomas of West Superior and T. B. Caldwell of Lanark, Ontario. 396 The American Geologist. one ae DEPARTMENT OF GEOLOGY AT THE UNIVERSITY OF WISCON- stn. Professor C. R. Van Hise, who has been at the head of this department for some years, was elected president of the university on April 2tst. His new duties begin about October Ist; in the meantime he is expecting to visit Hurope and attend the International Congress of Geologists at Vienna. Dr. C. K. Leith has been promoted from assistant professor to professor of structural and economic geology. Dr. Wm. H. Hobbs con- tinues as professor of mineralogy and petrology. Dr. J. Mor- gan Clements has resigned his professorship and will probably open an office as consulting economic geologist in New York City. Dr. N. M. Fenneman, of the University of Colorado, has been elected professor of general and physiographic geology. THE COMPLETION OF THE PALEONTOLOGIC MONOGRAPHS be- gun by the late O. C. Marsh has been entrusted to professor Henry Fairfield Osborn, vertebrate paleontologist of the Unit- ed States Geological Survey. The materials left by professor Marsh did not include any completed manuscript, but consist- ed chiefly of a series of fine lithographic plates and wood en- gravings, illustrating four important groups of vertebrates. The specimens illustrated are contained in part in the collec- tions of the Survey and in part in those made for the Yale University Museum under the direction of professor Marsh. In order to insure the completion of these monographs within a reasonable period, professor Osborn recommended to the Dt- rector of the Survey a division of authorship, assigning the monograph on the Ceratopsia to Dr. J. B. Hatcher, now con- nected with the Carnegie Museum, Pittsburg, and that on the Stegosauria to Dr. F. A. Lucas, of the United States National Museum. Professor Osborn has himself undertaken the prep- aration of the monographs on the Titanotheres or Brontother- idee and on the amphibious dinosaurs of the order Sauropoda. Unirep STaTEs GEOLOGICAL SuRvEy. The mineral re- sources of the Mount Wrangell district in Alaska will be dis- > cussed in Professional Papers No. 15 by Messrs. W. C. Men- denhall and F. C. Schrader. This report is now in press. The chief mineral resources of the district are copper, gold and ° coal. Dr. H. E. Gregory, of Yale University, has undertaken an investigation of the underground waters of Connecticut.” A topographic map of the country adjacent to the Rands- burg and Johannesburg districts of California will soon be issued. The district is a desert area, and its mineral wealth consists of gold. Hydrologic work consisting of the investigation of under- ground waters, has recently been begun in Michigan. Mr. W. F. Cooper, working under the supervision of Dr. A. C. Lane, state geologist, has “charge of the work. ae Personal and Scientific News. 397 Messrs. G. F. Becker, S. F. Emmons, and C. R. Van Hise have been appointed delegates to the International Congress of Geologists at Vienna. Dr. Arthur C. Spencer is to spend the present field season in Alaska, investigating the geology of Douglas island and making a special study of the ore deposits of the Treadwell mine. AMERICAN INSTITUTE OF MINING ENGINEERS. The meet- ing of the Institute arranged for July in British Columbia, with an excursion to Alaska, will not be held. The library of the Institute, located at the secretary’s office, No. 99 John street, New York City, comprises about 10,000 volumes, having been recently enriched by the deposit of the books of R. W. Raymond and of the libraries of the late Clar- ence King and R. P. Rothwell. These volumes, combined with the large list of technical papers and government reports owned by the Institute, make a very valuable collectian of literature on geology, mining, metallurgy and the allied arts. It is felt that the library, already possessing such a fine nucleus, should be made a complete reference library for the profession, and with that end in view it is proposed to raise a fund of $25,000 for the acquisition of additional books and for proper cata- loguing. If a sufficient amount is raised, it will be possible to publish and forward to members of the Institute a complete classified index of the library and to engage a librarian compe- tent to hunt up and abstract reports for members. This will be of special service to engineers remote from libraries. The important libraries of the late Clarence King and R. P. Roth- well, above mentioned, have been secured through the generos- ity of Mr. John Hays Hammond, and at his request will be known as the “Raymond memorial library.”’ WISCONSIN GEOLOGICAL AND NATURAL HISTORY SURVEY. The geological work of the survey for the coming summer will be along the following lines: 1. Dr. Samuel Weidman, assisted by Mr. W. D. Smith of the University of Wisconsin, is to spend the earlier part of the season in a study of the district about Baraboo where recent developments have shown the existence of deposits of hematite in a slate or iron-bearing formation which overlies the Baraboo quartzite. 2. Later in the season Messrs. Weidman and Smith will return to the area of crystalline rocks in the north-central part of the state (vicinity of Wausau) with the expectation of com- pleting the work in this district for a report on the general geology and also on the glacial features. 3. Professor U. S. Grant of Northwestern University will continue work in the lead and zinc district of the southwestern corner of the state, a preliminary report on which has just been published (Bulletin No. IX). He will be assisted by Messrs. 398 The American Geologist. Tune E. F. Burchard, E. E. Ellis and M. J. Perdue, of Northwestern University, and E. T. Hancock, of the University of Wisconsin. During the summer it is expected that detailed large scale topographic and geologic maps will be made of some of the more important mining centers. 4. Investigations on the clays of the state will also be car- ried on. A report on highway construction in the state (Bul- letin No. X) written by Dr. E. R. Buckley, now state geolo- gist of Missouri, has been recently published. THE INTERNATIONAL CoNGRESS OF GrEoLocrsts will hold its ninth session, Aug. 20 to 27th, 1903, inclusive, in the city of Vienna. The executive committee has chosen Mr. Max v. Gutmann, professor of mines at Vienna, as treasurer in place of Mr. F. Karrer, resigned. The membership being limited the committee appeals to geologists and others, in every land, who are especially inter- ested in geological subjects to attend the sessions so far as possible. The membership fee for this session has been fixed at twenty-one francs. This sum should be sent to professor Max von Gutmann, Kantgasse, Vienna, Austria. Those desiring to take part in the Congress, who shall have sent the registra- . tion fee will receive a certificate of membership and, later, the published transactions of the session. In making the program the committee has consulted lead- ing scientists in Europe and America and believe that the pa- pers and the discussions thereon will modify some current ideas upon the great problems of geological science. Excursions —The committee offers some fourteen different excursions to take place either preceding or immediately fol- lowing the session. Each of these will be under the guidance of a noted specialist in the field chosen. Those who desire to participate in these excursions are urged to send their names as soon as possible so that the com- mittee can make necessary arrangements for their comfort. The Geological Society of Hungary sends out a special in- vitation circular to the members of the congress to visit Buda- pest and the Danube. The excursion given on “the lower Dan- ube will be limited to r00 persons. Those desiring to take this excursion should make application before June 15 to the gen- eral secretary, C. Diener, Vienna, Austria. Tue NarionaL ACADEMy oF ScrIENcES held its Annual spring meeting in the National Museum April 20 to 23. Five new “members were elected bringing the total up to ninety-two. These five were: Professor Thomas C. Chamber- lain, University of Chicago, geologist; Professor William James, Harvard University, psychologist ; Professor Arthur G. Webster, Clark Universitv, Worcester, Mass., physicist ; Personal and Scientific News. 399 Professor Horace L. Wells, Yale University, chemist; Profes- sor Edward L. Mark, Harvard University, biologist. Below is the list of papers read: “An estimate of the weight of the skeleton in the Sauro- poda, or in the Sauropodous Dinosaurs,’ Henry F. Osborn; “New characters of the skulls of Carnivorous and Herbivor- ous Dinosaurs,’ Henry F. Osborn; ‘Models illustrating the evolution of the Amblypoda, also of the Dinosaur Diplodocus, together with the theory as to the habits.of the Sauropoda,” Henry F. Osborn; “Radioactivity of Thorium minerals,” Geo. F. Barker; ‘“The Law of Catalysis in concentrated solutions,” J. M. Crafts; “The standardization of thermometric measure- ments,” J. M. Crafts; The Rumford Spectroheliograph of the ‘Yerkes Observatory,” George E. Hale; ‘The determination of standard right-ascensions free from the personal equation for ‘star-magnitude” (with stereopticon illustrations), Lewis Boss; “On the semi-diurnal tide of the northern part of the Indian ocean,” R. A. Harris, introduced by Cleveland Abbe; “The melting point of a simple glass,” Arthur L. Day, introduced by G, Fe.Becker ; Biographical memoir of J. E. Holbrook,” \The- odore Gill; “Biographical memoir of Matthew Carey Lea,” George F. Barker; “Biographical memoir of Clarence King,” S. F. Emmons; “Biographical memoir of A. A. Gotild,” -Jeff- ries Wyman, read by W. H. Dall; “Biographical memoir of James E. Keeler,” Charles S. Hastings : “The diffusion of va- por into nucleated ait Cath: Barts5." ‘Biographical memoir of Theodore Lyman,” H. P. Bowditch; “The nomenclature of the topography of the bottom of the oceans,” Alexander Agassiz. GEOLOGICAL SocIETy oF WASHINGTON. At the meeting of May 6th the following program was presented: “Correlation of the Potomac Formation in Maryland and Virginia,” Lester F. Ward; “Pocono Rocks in the Allegheny Valley,” M. R. Campbell; “Age of the Mercer Group,” David White. The special meeting of May 13th, 1903, was devoted to a considera- tion of “The Quantitative Classification of Igneous Rocks,” continuing the discussion of the papers presented at the r4oth meeting. An abstract of Dr. Mathews’ paper is here given, which served as a basis for this discussion. Abstract of Dr. E. B. Mathews’ Criticism of the Quantitative Classification of Igneous Rocks. I. Strong points of the classification. I. Simplicity of the basal conceptions. There is no diffi- culty in grasping the basal conceptions which are applied with uniformity, and the rules for computation may be followed without the introduction of personal equation. 2. Sharpness of definition. The quantitative character of the classification produces sharpness in definition, leaves no ex- cuses for ambiguity, and enforces exact use of terms. The 400 The American Geologist. | ip system is expansive for increasing refinement and yet the num- ber of terms for a given rank or “division is limited. 3: Nomenclature. This is particularly strong in such terms as salic, femic, etc., and in the mnemonic terminations indicat- ing classes, ranks, ete. 4. Suggestive of new lines of investigation. The new grouping will stimulate a study of the model variations of a given form. It forces home the chemical composition and its mineralogical expression and emphasizes the complementary roles of rock-forming minerals. It will develop more careful descriptive work. Il. Weak points in the classification. t. Nomenclature. There is little connection between the field terms proposed and those of the new classification and they are based in some degree on different principles. The roots chosen, while adaptable to the specialists of today, have little or no meaning or arrangement for the new student or lay- man in petrography. 2. Subordination of texture. The new classification lays too little stress on the textures, which are easily recognizable. 3. Previous literature is rendered unavailable for a number of years until it has been thoroughly reworked and rephrased. 4 Chemical analyses. (a) Little can be told with certainty regarding the classifi- catory position from an inscription of a chemical analysis and no rock is surely placed without going through the entire com- putation. (b) The increased refinement in the discrimination between bulk analyses surpasses the ability to discriminate types in the field. This leads possibly to incorrect geological and petro- graphical interpretations of rock bodies. (c) The great expense involved in chemical analyses is like- ly to limit petrography to members of official organizations and men of means or leisure. The average petrographical worker of today among teachers can not command numerous high- class silicate analyses. (The use of slides removes in great measure this criticism. ) 5. The five-fold division vitiates the underlying principle of the classification in that the rock may be classified on 37.6 of the contents disregarding 62.4 of the same. This difficulty is most manifest in the Salfemanes although the rocks known introduce few major difficulties. Ill. Conclusion. The new classification will not in itself supplant the present nomenclature, but will furnish a means of expressing concisely the chemical position of a given rock in much the same way as the scientific nomenclature of botany is related in the pres- ent popular terms. INDEX TO VOL. XXXI. A. Alden, William C., 255. Alkaline rocks, Madagascar, croix, 183. America, how long ago peopled, 312. American Institute of Mining En- gineers, 65, 397. Ames knob, North Haven, Maine; a seaside note, Bailey Willis, 159. Ami, H. M. Sketch of the life and work of the late A. R. C. Selwyn, director of the Geological Survey of Cairada, 1869-1894; 1; and bibli- ography, 16. Americam Association for _vancement of Science, 66. Analyses en bloc et leur interpreta- tion, M. F. Fouque, 181. Anorthosyte, The rock name, C. F. Kolderup, 392. Apatite crystals, N. Knight, 62. Ashley, George H., 255. A. La- the Ad- Antwerp, N. Y., B. Babcock, B. G., North Dakota Geo- logical Survey, 383. Bain, H. Foster, 128, 394. Barrell. Joseph, 325. Basin-range structure in the Death Valley region of southeastern Cal- ifornia, M. R. Campbell, 311. Bauer, L. A., Magnetic declination tables, ete., 123. Belly River beds of Canada, J. B. Hatcher, 369. Berkey, C. P., 394. Bison, extinct, from Alaska, 262. Block mountains in New Mexico, D. W. Johnson, 135. Bownocker, J. A., The central Ohio natural gas fields, 218. Burchard, Ernest F., 394. Cc. Calkins, F. C., Petrography of the John Day basin, 54. Calin, S. Iowa Geological Survey, Cambrian faunas, G. F. Matthew, 256. Campbell, M. R. 255; Basin-range structure in the Death Valley reg- ion of southeastern California, 311, Cause of the Glacial period, H.-L: True, 384. Cayeux, L., Mesozoic formations in Greece and Crete, 386. Central Ohio natural gas fields, J. A. Bownocker, 218. Ceratops beds, Lance Creek, Wy- oming, J. B. Hatcher, 369. Chamberlin, T. C., 193, 394; Pleis- toceme geology near Lansing, Kan- sas, 265. Chester, Albert H., 394. Chicago Academy of Science, 64. Clapp, F. G., The maril-loess of the lower W) abash valley, 158. Clark, W. B., Maryland Geological Survey, 54. Clarke, John M., Annotations of Jaekel’s theses on Orthoceras and other cephalopods, 216. Clayton stone axe, 193. Columbia University, fall excursions of the geological department, H. W.. Shimer, 62. Concannon farm, Pleistocene geol- ogy of, near Lansing, Kansas, N. El Winchell, 263. Condra, G. E., On Rhombopora lepi- dodendroides (Meek), 22; An old Platte channel, 361. Cope, Edward D., catalogue of all the publications of, 1859-1897, P. Frazer, 180. ; Correspondence. Apatite crystals, Antwerp, N. Y., N. Knight, 62; Fall excursions of the geological pepe tment, Columbia University, H. . Shimer, 62; The rock name an- b orthosyte, C. F. Kolderup, 392. Crete, Jurassic and Cretaceous for- mations in, Li. Cayeux, 386. Curtis, George Carroll, Note on the West Indian eruptions of 1902, 40. Cushing, H. P., Recent geologic work in Franklin and St. Law- rence counties, N. Y., 180. D. Dale, T. Nelson, Structural details in the Green Mountain region and in eastern New York, 58. Davis, W. M., 262. Death Valley region of southeastern California, basin-range structure in, M. R. Campbell, 311. Determination of the feldspars in thin section, J. E. Spurr’ 376. Diamond mines of South Africa, 51. Diller, J. S. Topographic develop- ment of the Klamath mountains, 257. 402 Index. Ee Editorial Comment. The diamond mines of South Af- rica, 51; A new building for the national museum at Washing- tow, 178; How long ago was America peopled? 312. Ellensburg (Washington) folio, geo- logical atlas of U. S., G. O. Smith, 255. Erratic Bowlder from the coal mea- sures of Tennessee, S. W. McCal- lie, 46. Feldspars, determination in thin section, J. E. Spurr, 376. Fenneman, N. M., Lakes of south- eastern Wisconsin, 185. Foerste, Aug. F., The Richmond group along the western side of the Cincinnati anticline in Indi- ana and Kentucky, 3338. Fe Fouque, M. F., Les analyses en bloc et leur interpretation, 181. Frazer, Persifor, Alphabetical cross- reference catalogue of all the pub- lications of Edward D. Cope, 1859- 1897, 180. Fuller, M. L., The marl-loess of the lower Wabash valley, 158; Ditney folio, U. S. Geological Survey, 255. G. Gannett, Henry, The origin of cer- tain place names in’ the United States, 186. Gentil, Louis, Esquisse stratigra- phique et petrographique du pas- sin de la Tafna (Algeria), 253. Geological age of the West Indian yoleanic formations, J. W. Spen- cer, 48. Geological Society of America, 66, 128. Geological Society of London, 129. Geological Society of Washington, 64, 193; 325, 399. Geology of the Jemez-Albuquerque region, New Mexico, A. B. Rea- gan, 67. George, Russell D., 394. Glacial geology of New Jersey, R. D. Salisbury, 316. Glacial period, cause of, H. L. True, 384. Glacier lakes in the Cleveland hills, P. F. Kendall, 124. ; Grabau, Prof. A. W., 325. Greece, Lower Cretaceous in, L. Cayeux, 386. Gregory, H. E., 396. Grénwell, K. A., Bornholms Para- doxideslag og deres fauna, 186. H Hague, Arnold, 325. Hall, Prof. Charles M., The life and work of, by W. Upham, 195. Harris, Gilbert D., Report on the geology of Louisiana, 256. Harris, Israel H., Collection of in- vertebrate fossils in the 5 National Museum, C. Schuchert, TST: Harvard University, field course in geology, 262, 326. Hatcher, J. B., Relative age of the Lance Creek (Ceratops) beds of Converse ‘county, Wyoming, the Judith River beds of Montana, and the Belly River beds of Can- ada, 369. Hershey, Oscar H., Some evidence of two glacial stages in_the Kla- math mountains in California, 139: Structure of the southern portion of the Klamath moun- tains, 231, Hovey, Dr. EB. O., 193. Huntington, Ellsworth,’ 326. Index animalium, C. D. Sherborn, 184. , International Congress of Geologists at Vienna, 397, 398. Iowa Geological Survey, annual re- port, 124, J. Jaékel’s theses on the mode of ex-. istence of Orthoceras and other | cephalopods, R. Ruedemann, 199. John Day basin, petrography, F. C. Calkins, 54. Johnson, Douglas W., Block moun- tains in New Mexico, 135. eee River beds, J. B. Hatcher, 69. ; K. Kemp, James F., 193. Kendall, P. F., Glacier lakes in the Cleveland hills, 124. Klamath mountains, California, Os- car H. Hershey, 139, 231; topo- graphic development, J. S. Dil- ler, 257. Knapp, George N., 316. Knight, Nicholas, Apatite crystals, Antwerp, IN: Y., 62: Kolderup, C. F., The rock name an- orthosyte, 392. Kiimmel, Henry B., Geological Sur- vey of New Jersey, 316. EE Lacroix, A., Les roches volcaniques de la Martinique, 55; Les roches alealines, Madagascar, 183. Lance Creek (Ceratops) beds, J. B. Pera es 369. akes of southeastern Wisconsi igtie Bile Fenneman, 185. =e Lansing, Kansas, Valley loess and the fossil man of, Warren Upham, 25; Pleistocene geology of the Concannon farm, near, N. H Winchell, 263. ; pee Cm Ke 395. eonard, A. G., Iowa i Survey, 124. : Se oaical * ~~ Index. Louisiana, Report on geology, Gob: Harris, 256. M. McCallie, S. W., An erratic bowlder from the coal measures of Tenne- ssee, 46. Magnetic declination tables, etc., L. A. Bauer, 123. Mammoth’s tooth, 262. Manlius formation of New York, C. Schuchert, 160. Marl-loess of the lower Wabash val- ley, M. L. Fuller and F. G. Clapp, 158. Martinique volcanic rocks, A. La- eroix, 55. Maryland Geological Survey, W. B. Clark, 54. Mathews, E. B., Quantitative clas- sification of ignieous rocks, 399. Matthew, G. F., Notes on Cambrian faunas, 256. Merrill, G. P., A newly-found met- eorite from Mount Vernon, Chris- tian county, Kentucky, 156; cen- sus statistics, 193. Meteorite, Bath Furnace, Ky., 64. Michigam, topographical map, 395. Minerals observed on buried Chi- nese coins of the seventh century, Austin F. Rogers, 43. Moberg, John C., 53, 316. Monthly Author’s catalogue of Am- erican geological literature, 59, 125, 188, 259, 319, 386. Morse on living Brachiopods, C. Schuchert, 112. N. National Academy of Sciences, 398. National Museum, new building, 178. Natural gas fields; central Ohio, G. A. Bownocker, 218. New Jersey Geological Survey, Gla- cial geology, R. D. Salisbury, 316. New Mexico Academy of Sciences, 65; School of Mines, 129, 395. Newly-found meteorite from Mount Viernon, Christian county, Ken- tucky, G. P. Merrill, 156. Noetling on the morphology of the Pelecypods, R. Ruedemann, 34. North Dakota Geological Survey, E. EBs Babcock, and F. A. Wilder, VOv. Note on the West Indian eruptions of 1902, George C. Curtis, 40. Note om titaniferous pyroxene, A. N. Winchell, 309. oO. Ghio natural gas fields, J. nocker, 218, Origin of certain place names in as United States, Henry Gannett, - 186. Crthoceras and other cephalopods, Jaekel’s theses on the mode of ex- istence of, R. Ruedemann, 199. Ortman, A. FE., 324. Osborn, H. F., 369, 396. Al. Bow- 403 P. Peet, Charles E., 316. Perkins, G. H., Report on the ge- ology of Vermont, 122. , Petrography of the John Day basin, F. C. Calkins, 54. Platte channel, An old, G. E. Con. dra, 361. Pleistocene geology of the Concan- non farm, near Lansing, Kansas, N. H. Winchell, 263. Powell, John, Wesley, by G. P. Mer- rill, 327. Professional papers, 64, 396; United States Geological Survey, divis- ion of hydrology, 194; atlas foli- OS, 255. Pumpelly, Raphael, 262. Q. Quantitative classification of igne- ous rocks, E. B. Mathews, 399. R. Reagan, Albert B., Geology of the Jemez-Albuquerque region, New Mexico, 67. Relative age of the Lance Creek (Ceratops) beds of Converse county, Wyoming, the Judith River beds of Montana, and the Belly River beds of Canada, J. B. Hatcher, 369. Rhombopora _ lepidodendroides (Meek), G. E. Condra, 22. Richmond group along the western side of the Cincinnati anticline in Indiana and Kentucky, A. F. Foerste, 333. Rogers, Austin F., Minerals ob- served on buried Chinese coins of the seventh century, 43. Ruedemann, R. Noetling on the morphology of the Pelecypods, 34. Professor Jaekel’s theses on the mode of existence of Orthoceras and other cephalopods, 199. Russeli, Timber lines, 121; map of Michigan, 395. S Salisbury, R. D., Glacial geology of New Jersey, 316. Schuchert, €., Morse on_ living srachiopods, 112; The I. H. Har- ris collection of invertebrate fos- sils in the U. 8. National Museum, 1381; On the Manlius formation of New York, 160. Selwyn, A. R. C.,! Sketch of the life and work of the late, by H. M. Ami, 1; and bibliography, 16. Sherborn, C. D., Index animalium, 184. ° Shimer, H. W., Falll excursions of the geological department, Colum- bia University, 62; 193. Smith, G. O., Ellensburg (Washing- ton) folio, geological atlas of U. Si, 255: Some evidence of two glacial stages in the Klamath mountains in Cal- ifornia, O. H. Hershey, 139. Some results of the late Minnesota Geological Survey, N. H. Win- chell, 246, 404 Speneer, A. C., 397. Spencer, J. W., Geological age of the West Indian volcanic forma- tions, 48; 65. Spurr,’ J... ., The determination of the feldspars in thin section, 376. Structural details in the Green Mountain region and in eastern New York, T. Nelson Dale, 58. Structure of the southerm portion of the Klamath mountains, Callifor- nia, O. H. Fiershey, 231. T. Timber lines, I, C. Russell, ilPAle Tin in Alaska, 325. Titaniferous pyroxene, A. N. Win- chell, 309. Todd, J. E., Pleistocene geology near Lansing, Kansas, 291. Todd valley, an old Platte channel, G&. B. Condra, 361: True, H. L., The cause of the Gla- cial period, 384. U. Upham, Warren, Valley loess and the fossil man of Lansing, Kan- sas, 25; The life and work of Pro- fessor Charles-M. Hall, 195. Vv. Valley loess and the fossil man of Lansing, Kansas, Warren Upham, OF 40. Index. Van Hise, C. R., 129, 324, 394, 395. Vermont, Report of the state geolo- gist, G. H. Perkins, 122. Ww. Wahner, F., Das Sonnwendgebirge im Unterinnthal, 185. Washington state geological survey, 325. West Indian eruptions George C. Curtis, 40. West Indian volcanic formations, J. W. Spencer, 48. Whiteaves, J. F., 262. Wilder, F. A., North Dakota Geol- ogical Survey, 383. Willard, D. E., 192. Willis, Bailey, Ames knob, North Haven, Maine, a_ seaside note, 159; expedition to China, 394. Williston, S. W., 291, 3871. Winchell, Alexander N., Note on ti- taniferous pyroxene, 309. Winchell, Horace V., 324, 394. Winchell, N. H., Some results of the late Minnesota Geological Survey, 246; The Pleistocene geology or the Conicannon farm, near Lans- ing, Kansas, 263; explorations in Montana, 394. Wisconsin Academy of Arts, and Letters, 129. Wisconsin Geological and Natural History Survey, 397. Wisconsin, University of, ment of geology, 396. Wright, G. F., Pleistocene geology near Lansing, Kansas, 294. ; of 1902, Science, depart- iA il 52679 mi 3 011 IN 19 20 72 a - weer T 3 * - Nor. ae := . S ee an ok Pleo Se = - , . % . _ Sw = Ae. nw Y mal ees 5 f aoe 4 a - = oe S=—- eas a . : . - 4 = es ’* > 3 ae 7 & . a < e A te nt #1