UNIVERSITY OF ILLINOIS LIBRARY 6 Volume ® Je 06-10M Return this book on or before the Latest Date stamped below. A charge is made on all overdue books. Seem University of Illinois Library Cle £r \ PETES CTY OmpE DEO, CREATE , - ’ pale BMERICAN GEOLOGIST: A MONTHLY JOURNAL OF GEOLOGY AND ALLARD SCIENCES Editor: N. H. WINCHELL, Ainneapolis, Minn. ASSOCIATE EDITORS: FLORENCE Bascom, Bryn Mawr, Pa. SAMUEL CALVIN, Jowa City, Jowa. JOHN M. CLarRKE, Albany, N. Y. HERMAN L. FAIRCHILD, Rochester, N. Y. PERSIFOR FRAZER, Philadelphia, Pa. ULyssEs S. GRANT, Avanston, Jil. OLIVER PERRY Hay, Mew York, XN. Y. GEORGE P. MERRILL. Washington, D.C. CHARLES S. PROSSER, Columbus, Chio. WARREN UPHAM, S?. Paul, Minn. IsRAEL C. WHITE, Morgantown, W. Va. HORACE V. WINCHELL, Butte, Montana. VOLUME XxXXxVI JuLy TO DECEMBER, 1905 MINNEAPOLIS, MINN, THE GEOLOGICAL PUBLISHING Co. 1905 ey ard We io eTOED SO vr (eren wh AV a ' Digitized by the Internet Archive in 2010 with funding from University of Illinois Urbana-Champaign http://www.archive.org/details/panamericangeolo361905desm CONTENTS. JULY NUMBER. CiareNce LutHer Herrick. [Portrait], W. G. Tight.......... Tue Hicw AttirupE Conopiain. [Plate II]. Ida H. Ogilvie.. GENETIC AND STRUCTURAL RELATIONS OF THE IGNEOUS ROCKS OF THE Lower NEponseT VALLEY. [ Part I]. W. O. Crosby.... EpitorIAL COMMENT. Another meteorite in the Supreme Court.................. Review oF RECENT GEOLOGICAL LITERATURE. Contributions to Devonian paleontology, 1903, H. S. Wil- liams and E. M. Kindle, 49. Bearing of some paleontological facts on nomenclature and classification of sedimentary for- mations, Henry Shaler Williams. .........0.0.0cccccceecee MontHiy AvuTHor’s CATALOGUE OF AMERICAN GEOLOGICAL LIr- SMe MAMMA 4 PREC 2 Eh, share, oa arena eA clio Ge doors on am cfc wid Coo S ae CoRRESPONDENCE. Estimation of the silica in the Bedford limestone, Nicholas LEPINE Sob BiG ARO BBR AE eS OR OE Re bree PERSONAL AND ScIENTIFIC NEws. AUGUST NUMBER. Apert A. WricutT, G. Frederick Wright. [Portrait, Plate III.] GENETIC AND STRUCTURAL RELATIONS OF THE IGNEOUS ROCKS OF THE Lower NEPONSET VALLEY, MaAssAcuusetts, [II], W. O. IG ee ee HEARERS eae STRATIGRAPHY OF THE EASTERN OUTCROP OF THE Kansas PER- MIAN, J. H. Beede and E. H. Sellards, [Plates IV and V].. THE FUNDAMENTAL COMPLEX BEYOND THE SOUTHERN END OF THE ROG UMOUMPAINS. GHGS: Ie. IGEYES. icc cciereisoloe co neeses wes Review oF RECENT GEOLOGICAL LITERATURE. The Two Islands and what came of them, Thos. Condon, 122; Ice or Water: Another appeal to Induction from the scholastic methods of modern Geology, Sir Henry H. Howorth, 125; The rocks of Tristan d’Acunha brought back by H. M. S. Odin, 1904, with their bearing on the question of the permanence of ocean basins, FE. H. L. Schwartz, 126; Geological Survey of New Jersey, Annual report for the year 1904, Henry B. Kiimmel, 126; The Geology of the Perry basin in southeastern Maine, Geo. O. Smith, and David White, 127. Monturty AvutHor’s CATALOGUE OF AMERICAN GEOLOGICAL Lit- 93213 34 47 49 AYs II2 ted SEPTEMBER NUMBER. PLEISTOCENE FEATURES IN THE SYRACUSE REGION, H. L. Fairchild, fu sttes Wi lecariael as Vall) site eaten enz area as etonah noes Reena ere a a Notes ON THE PERMIAN FORMATIONS OF Kawnsas, Charles S. PGS SBI Mee wee Mad coos endes stale es erences roe atte este Re Se ice < Tue AtLtantic HicHLANDS SECTION OF THE New JERSEY CRE- racic, J. K. Prather, [Plates VIII, IX, X]c2..-ss7258 Blacher. cectege wereancie imo tee satel ais MontuHty AurHor’s CATALOGUE OF AMERICAN GEOLOGICAL LIT- ERATURE (ce c%s acne sco no or Ore one Oe een een ees ote enna The American Geologist. December. 1905. 135 143 162 179 188 199 230 244 250 261 262 Index, Volumes I-XXXVI. i CoRRESPONDENCE. Economic Geology in Peru, V. F. Marsters, 265; Mateo OOO aio, Ciera 5 bia, s.'s bao 'e 6.25 00 'Gie, «erable, 5 av te 5% 266 Pee ATA, SCIENTIFIC NEWS ~ 00% 0c 200 csc d ens veces veleles 267 NOVEMBER NUMBER. GiactAL MovEMENTS IN SOUTHERN SWEDEN, G. F. Wright, Vis enicid stk anc wilan sa Gciee .e bo nelee os eves 269 Botson PLAINS OF THE SOUTHWEST, W. G. Tight............... 271 GLACIAL LAKES AND MARINE’ SUBMERGENCE IN THE HvupDSON PAAMPLATN VALLEY, Warren Uphant ...2.....0020ceeteuneee 285 - THE JURASSIC HORIZON AROUND THE SOUTHBRN END OF THE ROCKY AMMAR TE ROE IC OMEN ng vial Sa tasclae Vac ce es bee ob eee we 289 Biesinsrruro GEouocicA DE Mexico, F..N. Guild.........2000 00% 203 SERPENTINES IN THE NEIGHBORHOOD OF PHILADELPHIA, Anna J. UPR oye ete tas hte ES ITS Sy Als >, Glove now #0 wes Die 206 AN EXPLANATION OF THE PHENOMENA SEEN IN THE BECKE METH- OD OF DETERMINING INDEX OF REFRACTION, IV. O. Hotchkiss... 305 Consolidation of the GroLocist with “Economic Geology’... 309 Review oF RecENT GEOLOGICAL LITERATURE. The secondary origin of Certain Granites, R. A. Daly, 312; La Montagne Pelée et ses eruptions, A. Lacroix, 316; Min- erals in Rock Sections: the practical methods of determining them with the microscope, L. M. Luquer, 319; Geology of Western ore deposits, Arthur Lakes, 319; Grundztige der Gesteinskunde, Teil I and II, Ernest Weinschenck, 319; Structural and Field Geology, James Geikie, 320; Economic Geology of the United States, Hemrich Ries, 321. Montuty AvutTHor’s CATALOGUE OF AMERICAN GEOLOGICAL Lit- “Ra DINE Sg eBly ie Srp eo aE era gee nae 2 323 CoRRESPONDENCE. Per OrMIPeTONS GeENETA Vy eacea sti style oe vee ws oa ae eae 330 LARSON eA TDS CLON TERT CR INE WIS! ics seiniscttinaln sess slelersi St era's’ oles 331 DECEMBER NUMBER. Cun Ar iNnex, Volumes: Ito: XOORVL oo fie ce dew de ce ese es 333 a ae A ST SE EY PT DB ES Errata, Vor. XXXVI. Page 320, line 6, for “comparisons” read companions. Page 332, line 4 from the bottom, for “62” read 26. oane ‘ 4 r i oy ie _ a (7% es 4 \ - ‘ - ' PAs « "dl “a ee vd of a 2 . pt One ey r Gr * oi eG ae a A MAL as ®) U s% nil y be eh ew were he aeet MEET oS wis ate f ‘ < oy = f os > my tan at. Sy je ae een a de a 7 =" a 4 ; ~ WR wees Cat he eid ees Ne =~ "> nt - , ' : = LIBRARY rays FS See OF THE ete ciel. ¢ UNIVERSITY of ILLINOIS | ) ’ \ > \ - ra P . Y. THE AMERICAN GEOLOGIST, VoL. XXXVI. PLATE I The portrait of Dr. Herrick, vol XXXVI , plate 1, was badly printed. The binder will please substitute this. THE mote RICAN GEOLOGIST. VOL. XXXVI, JULY, 1005. No. I. CLARENCE LUTHER HERRICK. > By W. G. Tieut, Albuquerque, New Mex. PORDRATT, PLATE £- When a great and good man is taken from the midst of his life work and those whom he has served are called upon to realize their loss, there is ever a desire to perpetuate his memory and to preserve such knowledge concerning him as wiil be of further service to humanity. In preparing a fit memorial to Dr. Herrick the writer realizes his own inability to do justice to the man and his work. Perhaps no other outside of his immediate family was better ac- quainted with him than myself. Having lived with him in the home, in the camp, in the school room and laboratory and being in almost constant correspondence with him for a long term of years when circumstances separated us, his death is a very deep personal loss. Dr. Herrick has many pupils scattered over the world who feel that they owe much to him and in whom he took a very deep interest and pride. Of this large number there were two boys who were a little nearer to Dr. Herrick’s heart than any of the others. Not because they were any better or brighter but because of the circumstances connected with their coming together. These two were Herbert L. Jones and myself. When Dr. Herrick went to Denison university in 1885 and started his career as a teacher he was a compaiatively young man, be- ing only twenty-seven years old, but his characteristic earn- estness and enthusiasm were so manifest that he attracted _ to himself out of a graduating class of thirteen these two boys and through his influenee both remained at Denison for a year of post-graduate work. We were the first resident 2 The American Geologist. pct post-graduate students Denison ever had. Prof. Jones de- voted his life to the study of Botany, contributing several important articles to science. He taught science in the pre- daratory department of his Alma Mater for several years, was assistant botanist at Harvard for a time, resigning to accept the professorship of Botany at Oberlin college, where he served but one year, when called from his labors by Death, at the very opening of his career. It was because we two boys were first on his long list of devoted pupils that we were held with special regard by him. Yet in spite of the intimacy of my relations with him through all these years that have intervened it 1s with misgiving that I undertake the sad task of presenting this tribute to his life and character. In order that my views may not be colored too much by my own personal feeling and sense of personal apprecia- tion it is my purpose to express myself largely through the words of others and to present such views as have been given by them as will in my judgment bring out the salient features of Dr. Herrick’s life and work. In a letter written to Rev: J. L. Cheney,- Cleveland, Ohios Sepr, 27, 51904 brother C. J. Herrick says: “His was a life very difficult for any one person to estimate, for his work was in so diverse fields that few men have even a speaking acquaintance with all of them. His life may be roughly divided into four periods. Very early in his career he seems to have laid out at least in a rough way a rather ambitious plan of action including for the first part of his life miscellaneous research and study in the broad field of general natural history—a general broad foundation. Then was to follow a period of intense specialization in the circumscribed field of zoological work leading up to a mastery of anatomy, and physiological and comparative psychology on the basis of the mechanism of the nervous system and to the philosophical correlation. So far as I am aware my brother never announced this or any other program, and I doubt if such a thing was ever definitely formulated even in his own mind;. yet from some of his conversations which I remember years ago I believe that some such plan was in his mind. While the four peri- ods referred to above were marked by extraneous events, Clarence Luther Herrick—Tight. 3 apparently artificial or arbitrary, yet I think it may be said that the ideal scheme was in the end fairly achieved, though with great deviation in the details of the working.” FIRST PERIOD. 1858-1884. The son of a Baptist clergyman, Dr. Herrick was born near Minneapolis, Minn., June 21, 1858. He grew up ina home far from neighbors as a solitary child with few play- mates and very early showed his bent for the study of nature. - While still in the Minneapolis high school he col- lected extensively and left at graduation a case of over a hundred mounted bird skins and other specimens in the high school. It was during this period that his father got him an eight dollar microscope. With this crude instrument and without library facilities he worked over the fresh water fauna of the neighboring brooks and pools so thoroughly that before graduating from the university of Minnesota, in 1880, he had published several articles of value on the fresh. water crustacea of Minnesota and four years after gradua- tion, with somewhat better facilities, published a report on the microcrustacea of Minnesota which is still standard. These years and those of his university course were filled with many bitter struggles, not the least of which was with poverty and the lack of materials for study. But notwith- standing these, he completed his course in three years, at the same time partly supporting himself by assisting on the Minnesota natural history survey. He had also showed so obvious a native gift with his pencil that upon his gradu- ation the president of the university said that he was uncer- tain whether to advise him to devote his life to science or art. But there was no uncertainty in the mind of the young man. Continuing his work with the geological and natural history survey of Minnesota after graduation, he published many papers in rapid succession on the fauna of the state and began an extensive report, the first volume of which was completed in 1885. This was a large quarto on the mammals of the state fully illustrated with many colored plates and pen drawings. It was accepted for publication, but for lack of funds in the survey, never saw the light. Years afterward, in 1892, a small octavo was published by 4 The American Geologist. duly aCe the survey made up of the more popular parts of this work. He spent a year in Leipzig at the University during 1881- *82. And in 1883 he was married to Miss Alice Keith, of Minneapolis. He took his Masters and Doctors degree from the uni- versity of Minnesota. SECOND PERIOD. 1884-1889. Called to the chair of Geology and Natural History of Denison university, Granville, Ohio, in the summer of 1884, he spent the fall of that year at Denison, then returned to Minneapolis to complete the work begun by him on ‘the Minnesota survey and in the fall of 1885 moved with his family to Denison. It had been his intention to continue his zoological work there, and there was great activity in this line during the entire period, but the routine excursions made as a part of the instruction of his geology classes showed him so much of interest in the local strata that his chief labors while in Granville, were upon the fossils and stratigraphy of the Waverly free stones and shales of Ohio. This work was abruptly cut short by his removal from Gran- ville in 1889, and while never rounded out as he would have liked is probably his most important geological work. In 1885 he founded the Bulletin of the Scientific Laboratories of Denison university, in which the greater part of his re- searches and those of his pupils on Ohio geology were published. His phenomenal success as a teacher during this and subsequent periods was due to factors some of which are easily seen—others hard to define. After his attractive per- sonal qualities and magnetic enthusiasm I should place his deep philosophical insight and the fearless way in which he opened up his profoundest thinking to even his most ele- mentary pupils. The ability to do this without befogging the air was an exceedingly rare gift and was stimulating to even a dullard. He knew the philosophical classics thor- oughly from original sources and the trend of his thinking was very early foreshadowed in the translation of Lotze’s Outlines of Psychology, published in 1885 in Minneapolis, with its appended chapters on the nervous system. Clarence Luther Herrrick—Tight. 5 THIRD PERIOD. 1889-1894. Upon his acceptance of the chair of Biology in the uni- yersity of Cincinnati in 1889, the geological studies with which the preceding five years had been so fully occupied were summarily brought to a close and he threw himself with renewed energy into the study of the nervous system. Extensive papers on the brains of different animals appear- ed in rapid succession of which the most valuable are two series, one on the brains of various fishes, the other on those of reptiles. In 1891 the Jougnal of Comparative Neur- ology was founded and served as the medium of publication for most of these researches. The founding of this journal can best be designated as a piece of characteristic audac- ity. It was a purely private enterprise with no funds as- sured and very little outside co-operation promised. But without counting the cost he plunged boldly in, expecting a constituency to be developed as the work went on. In this he has not been disappointed wholly, though recognition of financial needs has lagged sadly behind that of the scien- tific excellence of the journal. At the close of 1891 he re- signed his chair in the university of Cincinnati to accept a chair of Biology in the university of Chicago, then being re- organized. The early part of 1892 was spent in Europe, chiefly in Berlin. Upon his return the adjustment at Chic- ago presented unexpected difficulties and after a series of misunderstandings he withdrew from the institution, declin- ing an offer to return. to Germany for further study on full salary. He was immediately elected to his old post in Denison university with an assistant and the privilege of devoting only a part of his time to teaching, the remainder to be spent either at home or abroad in the further prosecu- tion of his research. A Waverly Trilobite. Bul. Sci. Lab. Denison Univ. Vol. ie Part, 5 Some American Norytes and Gabbros. (With E. S. Clark and J. L. Deming). Am. Geol., Vol. I., No. 6. Science in Eutopia. American Naturalist, vol. xxii, pp. 698- 702. The Geology of Licking County, Ohio. Part III. and IV. The Subcarboniferous and Waverly groups. Bul. Sci. Lab. Denison Univ. Vol. III., Part I. Geology of Licking County. Part IV. List of Waverly Fos- sils, continued. Bul. Sci. Lab. Denison Univ. Vol. IV. Baniel Educational Briefs. Bul. Sci. Lab. Denison Univ. Vol. IV, Part, 1 i Lotze’s Ontology. The Problem of Being. Bul. Sci. Lab. Denison Univ. Vol. IV., Part II. Notes upon Waverly Group in Ohio. American Geologist, Vol. III., No. II. Investigation of the Waverly Group in Ohio. American Geologist, Vol. IiI., No. I. A Contribution to the Histology of the Cerebrum. The Cin- cinnati Lancet Clinic. N. S., vol. xxiii, pp. 325-327. Additions and Corrections to Miller’s North American Pale- ontology. American Geologist, Vol. V., No. 4. Notes on the Brain of the Alligator. Journal Cincinnati Society of Natural History. Vol. xii, pp. 129-162, 9 plates. Suggestions upon the Significance of the Cells of the Cere- bral Cortex. The Microscope, Vol. X., No. II., pp. 33-38, 2 plates. The Central Nervous System of Rodents. Preliminary Pa- per. (With W. G. Tight). Bul. Sci. Lab. Denison Univ., Vol. v, pp. 35-95, 19 plates. The Philadelphia Meeting of the International Congress of Geologists. American Naturalist, vol. v, pp. 379-388. The Commisures and Histology of the Teleost Brain. Anat. Anz. Vol. VI., No. 23-24, pp. 676-681, 3 Figs. Biological Notes upon Fiber, Geomys and Erethyzon. Bul. Sci. Lab. Denison Univ., Vol. VI., Part I. pp. 5-25. (With C. J. Herrick). The Cuyahoga Shale and the Problem of the Ohio Waverly. Bul. Geological Soc: of America, vol. ii, pp. 31-48, 1 pl. 22 1892 The American Geologist. aay LUOe The Evolution of the Cerebellum. Science, vol. xviii, pp. 188- 189. Contributions to the Comparative Morphology of the Central - Nervous System. I. Illustrations of Architectonic of the Cerebellum. Journ. Comp. Neur., vol. I., pp. 5-14, 4 plates. Contributions to the Comparative Morphology of the Central Nervous System. IJ. Topography and Histology of the Brain. of Certain Reptiles. Journ. Comp. Neur. Vol. I., pp. 14-37, 2 plates. : Laboratory Technique. A New Operating Bench. Jour. Comp. Neur. Vol. I., p. 88. Editorial. The Problems of Comparative Neurology. Journ. Comp. Neur., Vol. I., pp. 93-105. Notes upon Technique. Journ. Comp. Neur. Vol. I., pp. 133- 134. Contributions to the Comparative Morphology of the Central Nervous System. III. Topography and Histology of the Brain of Certain Ganoid Fishes. Journ. Comp. Neur. Vol. I., pp. 149-182, 4 plates. Editorial: Neurology and Psychology. Journ. Comp. Neur., Vol. I., pp. 183-200. Contributions to the Morphology of the Brain of Bony Fishes. (Part I. by C. Judson Herrick). Part II. Studies on the Brain of Some American Fresh Water Fishes. Journ. Comp. Neur., Vol. I., pp. 228-245, 3 plates, and pp. 3338-358, 2 plates. j The Mammals of Minnesota. A Scientific and Popular Ac- count of their Features and Habits. Bul. No. 7, Geol. & Nat. Hist. Survey of Minn., 300 pp, with 23 figures and 8 plates. Notes upon the Anatomy and Histology of the Prosenceph- alon of Teleosts. Am. Nat., vol. xxvi, No. 2, pp. 112-120, 2 plates. Additional Notes on the Teleosts Brain. Anat. Anz., vol. vii., No. 13-14, pp. 422-431, 10 figures. Notes Upon the Histology of the Central Nervous System of Vertebrates. Festschrift zum siebenzigsten Geburtstage Rudolf Leukharts, pp. 278-288, 2 plates. The Cerebrum and Olfactories of the Opossum, Didelphys virginica. Journ. Comp. Neur., Vol. II., pp. 1-20, and Bul. Sci. Lab. Denison Univ., Vol. VI., Part 2, pp. 75-94, 3 plates. A Contribution to the Morphology of the Brain of Bony Fishes. Part II. Studies on the Brain. of Some American Fresh Water Fishes. (Continued). Journ. Comp. Neur., Vol. II., pp. 21-72, 8 plates. Neurologists and Neurological Laboratories. No. 1. Prof. Gustav Fritsch, with portrait. Journ. Comp. Neur., Vol. II. The Psycho-Physical Basis of Feeling. Journ. Comp. Neur. Vol. II., pp. 111-114. 1893 1894 1895 Clarence Luther Herrick---Tight. 23 Instances of Erroneous Inference in Animals. Jour. Comp. Neur., Vol. 2, p. 114. Editorial: Instinctive Traits in Animals. Jour. Comp. Neur. Vols H.; pp: 115-136. Histogenesis and Physiology of the Neryous Elements. Jour. Comp. Neur., Vol. II., pp. 137-149. Intelligence in Animals. Journ. Comp. Neur., Vol. II., pp. 157-158. Embryological Notes on the Brain of the Snake. Journ. Comp. Neur., Vol. II., pp. 169-176, 5 pls. Localization in the Cat. Journ. Comp. Neur, Vol. II., pp. 190-192. ; The Scope and Methods of Comparative Psychology. Deni- son Quarterly, Vol. 1., pp. 1-10, 134-141, 179-187, 264-281. Articles in Wood’s Reference Hand Book of the Medical Sciences, Vol. [X.,sSuppl., as follows: (1) The Comparative Anatomy of the Nervous System. (2) The Histogenesis of the Elements of the Nervous System. (3) The Physiolo- gical and Psychological Basis of Emotions. (4) Waller’s Law. The Evolution of Consciousness and of the Cortex. Science, Vol. XXI., No. 543, pp. 351-352. The Development of Medullated Nerve Fibers. Journ. Comp. Neur., Vol. III., pp. .11-16, 1 plate. Editorial: The Scientific Utility of Dreams. Journ. Comp. Neur., Vol. III., pp. 17-34. The Hippocampus in Reptilia. Journ. Comp. Neur., Vol. III., pp. 56-60. ; Observations upon the so-called Waverly Group of Ohio. Ohio Geological Survey, vol. vii, pp. 495-515. * Contributions to the Comparative Morphology of the Central Nervous System II. Topography and Histology of the Brain of certain Reptiles (Continued). Journ. Comp. Neur., Vol. III., pp. 77-106, 5 plates, and pp. 119-140, 6 plates. Report upon the Pathology of a case of General Paralysis. Journ. Comp. Neur., Vol. III., pp. 141-162, and Bul. No. 1 of the Columbus State Hospital for the Insane, 5 plates. The Callosum and Hippocampal Region in Marsupial and ‘Lower Brains. Journ. Comp. Neur., Vol. III., pp. 176-182, 2 plates. The Seat of Consciousness. Journ. Comp. Neur., Vol. IV., pp. 221-226. How the Entomologist Saved the Party. Forest and Stream, Vol. 45, No. 18. Pockets. Forest and Stream. Vol. 45, No. 12. A Day with a Naturalist on a New Mexican Ranch. Forest and Stream, Vol. 45, No. 14. Synopsis of the Entomostraca of Minnesota, with Descrip- 24 1896 1897 The American Geologist. a tions of Related Species Comprising all known Forms from the United States included in the Orders Copepoda, Clado- cera, Ostracoda. Geol. & Nat. Hist. Survey of Minn... Zoological Series, II., pp. 1-525, 81 plates. (With C. H. Turner.) ‘ Microcrustacea from New Mexico. Zool. Anz., Vol. XVIII., No. 467. Modern Algedonic Theories. Journ. Comp. Neur., Vol. V, pp. 1-32. The Histogenesis of the Cerebellum. Journ. Comp. Neur., Vol. V., pp. 66-70. Notes on Child Experiences. Journ. Comp. Neur., Vol.: V., pp. 119-123. Editorial: The Cortical Optical Center in Birds. Jour. Comp. Neur., Vol. V., pp. 208-209. Editorial: Neurology and Monism. Jour. Comp. Neur., Vol. V., pp. 209-214. The Building Stones of Socorro, N. M. New Mexico Bureau of Immigration Papers, May. The Testimony of Heart Disease to the Sensory Facies of the Emotions. Psych. Rev., Vol. III., No. 3. Suspension of the Spatial Consciousness. Psych. Rey. Vol. Ill., No. 2, pp. 191-192. Focal and Marginal Consciousness. Psych. Rey. Vol. III., No. 2, pp. 193-194. The Psycho-sensory Climacteric. Psych. Rev., Vol. III., No. 6, pp. 657-661. The Critics of Ethical Monism. Denison Quarterly, Vol. IV., No. 4, pp. 240-252. The So-called Socorro Tripoli. American Geologist, Vol. 18, No. 3. Illustrations of Central Atrophy after Eye Injuries.. Journ. Comp. Neur. Vol. VI., pp. 1-4, 1 plate. Lecture Notes on Attention. An Illustration of the Employ- ment of Neurological Analogies for Psychical Problems. Journ. Comp. Neur., Vol. VI., pp. 5-14. Editorial: The Ethics of Criticism. Journ. Comp. Neur., Vol. VII., pp. 71-72. Psychological Corrollaries of Modern Neurological Discover- ies. Journ. Comp. Neur., Vol. VIII., pp. 155-161. Inquiries regarding Current Tendencies in Neurological Nomenclaturee. Journ. Comp. Neur., Vol. VII., pp. 162- 168. (With C. J. Herrick). The Propagation of Memories. Pysch. Rev., Vol. IV., No. 3. The Geology of a Typical Mining Camp. American Geologist, Volk XxX Non4: The Waverly Group of Ohio. Fin. Rep. Geol. Survey of Ohio. Vol. VIII. 1898 1899 1900 1901 Clarence Luther Herrick---Tig ht. 25 The Waverly Group of Ohio. Bul. Geol. Soc. of America. The Vital Equilibrium and the Nervous System. Science N. S., Vol. VII., No. 181, pp. 813-818. Physiological Corollaries of the Equilibrium Theory of Nervous Action and Control. Journ. Comp. Neur., Vol. VIII., pp. 21-31. The Geology of the Environs of Albuquerque, New Mexico. American Geologist, Vol. 21. The Somatic Equilibrium and the Nerve Endings in the Skin. Part I. Journ. Comp. Neur., Vol. VIII., pp. 32-56, 5 plates. (With C. E. Coghill). « Papers on the Geology of New Mexico. Bul. Hadley Lab. Univ. N. M., Vol. I., and Bul. Sci. Lab. Denison Univ.,. Vol. XI., pp. 75-92. The Cortical Motor Centers in Lower Mammals. Journ. Comp. Neur., Vol. VIII., pp. 92-98, 1 plate. The Occurrence of Copper and Lead in the San Andreas and Caballo Mountains. American Geologist, Vol. XXII, No. 5. Substitutional Nervous Connection. Science, N. S., Vol. VIIL., p. 108. Geology of the San Pedro and Albuquerque Districts. Bul. Hadley Lab. University of New Mexico.. Vol. I., and Bul. Sci. Lab. Denison Univ., Vol. XI., pp. 93-116. The Material Versus the Dynamic Psychology. Psych. Rey. Vol. VI., No. 2, pp. 180-187. Editorial: Clearness and Uniformity in Neurological Descrip- tions. Journ. Comp. Neur., Vol. IX., pp. 150-152. Notes on a Collection of Lizards from New Mexico. Bul. Sci. Lab. Denison Univ., Vol. XI., pp. 117-148, 11 plates. (With John Terry and H. N. Herrick, Jr.) Geography ‘of New Mexico. A Chapter in the Natural Ad- vanced Geography. .N. Y., Am. Book Co., 6 pp, map and 9 figures. Geology of the White Sands of New Mexico. Journ. Geol., Vol -Viil., INO: 2: Miscellaneous Economic Papers. Salt, Gypsum, Cement, Clays, Graphite, in New Mexico. Bul. Hadley Lab. Univ. of New Mexico, Vol. II. Identification of an Ohio Coal Measures Horizon in New Mexico. American Geologist, Vol. XXV, No. 4. Geology of the Albuquerque Sheet. Bul. Hadley Lab. Univ. of New Mexico. Vol. II., Part 1., and Bul. Sci. Lab. Denison Uniy., Vol. XI., pp. 175-239; 1 map and 32 plates. Report of a Geological Reconnaissance in western Socorro, and Valencia Counties in New Mexico. Bul. Hadley Lab. Univ. of New Mexico. Vol. II., Part I., and American Geolo- gist, Vol. XXV., pp. 331-346. Neurological Articles for Baldwin’s Dictionary of Philosophy 26 1903 1904 1904 1905 The American Geologist Say ee and Psychology, New York, The Macmillan Co. (With C. J. Herrick.) Articles on the Development of the Brain and on End-Organs, Nervous, in Wood’s Reference Hand-Book of the Medical Sciences, Second Edition, Vols. Il. and III. Secondary Enrichment of Mineral Veins in Regions of Small Erosion. Mining and Scientific Press, San Francisco, Vol. TG XEXEAV NOD iD Oe Laws of Formation of New Mexico Mountain Ranges. Am. Geol., Vol. XXXIII., pp. 301-312. Block Mountains in New Mexico. A Correction. American Geologist, Vol. XXXIII. The Clinoplains of the Rio Grande. American Geologist, Vol. XXXIII., pp. 376-381. Fundamental Concepts and Methodology of Dynamic Realism. Journ. Phil. Psy. Sci. Methods, Vol. I., No. II., 281-288. The Dynamic Concept of the Individual. Journ. Phil. Psy. Sci. Methods, Vol. I., No. 14, pp. 372-378. Editorial: L’Envoi. Journ. Comp. Neur. and Psych., Vol. XIV., No. 1, pp. 62-63. The Beginnings of Social Reaction in Man and Lower Ani- mals. Journ. Comp. Neur. and Psych. Vol. XIV., No. 2, pp. 118-124. Color Vision. (A critical Digest). Journ. Comp. Neur. and Psych., Vol. XIV., No. 3, pp. 274-281. Recent Contributions to the Body-Mind Controversy. Journ. Comp. Neur. and Psych.,-Vol. XIV., No. 5, pp. 421-432. A Coal Measure Forest near Socorro, New Mexico. Jour. of Geol., Vol. XII., No. 3, April-May, pp. 237-251. Lake Otero, an Ancient Salt Lake Basin in Southwestern New Mexico. Am. Geol., Vol. XXXIV., No. 3, pp. 174-189. The Logical and Psychological Distinction between the True and the Real. Psych. Rev., Vol. XI., No. 3. The Law of Congruousness and its Logical Application to Dynamic Realism. Journ. Phil. Psy. Sci. Methods, Vol. I., pp. 595-604. Mind and Body—The Dynamic View. «Psych. Rev., Vol. XI, pp. 3895-409. The Passing of Scientific Materialism. The Monist, Vol. XV, No. 1, pp. 46-86. (Followed by an Obituary by Dr. Carus, pp. 151-153.) — UgRARY _ UNIVERS|T ‘ “OFILLINOISurs ‘SNIVELNOOW ZILYO HHL TAXXX ‘IOA ‘LSI9010Gy) NVOINENY FHL aa ‘TI ALYIg The High Altitude Conoplain---Ogilvie. a7 THE HIGH ALTITUDE CCNOPLAIN; A TOPOGRAPHIC FORM ILLUSTRATED IN THE ORTIZ MOUNTAINS. By Ipa H OGILVIE, PH. D. RocKLAND, ME. PLATE II. During the past winter the writer was engaged upon a somewhat detailed survey of the Ortiz mountains, New ‘Mexico. These mountains are in the central part of the territory, some twenty-five miles east of Albuquerque, and somewhat farther southwest of Santa Fe. The region proved to be of unusual interest from the three separate points of view of physiography, petrography, and palzon- tology. A full report on all of these subjects will be pub- lished elsewhere, the present paper touching only upon cer- tain physiographic points of general interest. The Cordilleras of North America in Mexico and for one hundred or more miles north of Mexico, consist of many ranges. These ranges are various in length, hight and direction, hut the general trend of the Cordilleras as a whole is N. W.—S. E. The ridges are generally steep and are separated by flat plateaus. The general surface of the plateau region is rarely less than 6,000 feet in altitude, al- though in some cases rivers have. cut below the general level. Near the 34th parallel the Cordilleran belt divides, one portion trending northward, to and beyond Colorado, the other portion running westward and then northward through Arizona and Nevada. These form respectively the Rocky mountains and the Basin ranges. Between them lie the great plateaus. Bordering the Cordilleran country are many volcanic areas. The eruptions vary in age and in type, extending from shortly after the close of the Cretaceous to nearly recent time, and including volcanic cones, extrusive and in- trusive sheets, dikes, necks and laccoliths. The volcanic region is confined to the borders of the Cordilleran belts. The Ortiz mountains lie within this borderland, in the eastern branch, not many miles north of the point where the ranges fork. They are laccolithic in origin; post-Cre- taceous and probably pre-Pliocene in age. West of the 28 The American Geologist. oa ee Ortiz are the Sandia mountains, a range of the basin type whose steep western face marks a fault scarp with a throw of ever 4,000 feet. On the east the Sandias have a gentle slope and the beds dip gently east. The gentle easterly dip persists for many miles, and across the edges of these dip- ping beds a plain has been cut. The plain is not perfectly flat but has irregularities due to two causes. One of these is the Rio Grande and its tributary, Galistro creek, which have begun to dissect the plain; the other the difference in hardness of the various rocks cut, the edges of hard beds standing up in cuesta-like scarps. The hardest beds in the region are igneous sheets, derived from the Ortiz mountains. The Ortiz laccolith was intruded after the strata were tilted to the east. Its cover has-been largely removed by erosion, and the tops of the central and highest mountains (whose altitude is a little short of 9,000 feet) consist of the igneous core. Across the edges of the surrounding strata a plain has heen partly built and partly cut, this plain slop- ing away from the laccolith on all sides. Because of its outward slope in all directions this form is here named a conoplain, and its slope is partly cut and partly built. This conoplain becomes continuous below with the general level of the region, at an altitude of about 5,800 feet. The cono- plain has been cut alike across the Cretacic beds and the igneous sheets, and upon its surface has been deposited alluvial material (the Santa Fé marl of Hayden). It is not to be understood that this plain is a smooth surface with the configuration of a cone; on the contrary the harder beds stand above the soft to the extent of upwards of a hundred feet. But a line drawn from the central mountains outwards in any direction will pass over a surface cut on the sur- rounding rocks and sloping upwards towards the mountains. It is confidently believed that such a form is the normal one in a mountainous arid region, differences of topographic age being marked by differences in slope. The difference in altitude between the mountains and the surrounding plateau (a difference of about 4,000 feet) is sufficient to produce a marked difference in precipitation. Vegetation is the measure of precipitation. The mountains catch the rain, and are in consequence forest-covered, with The High Altitude Conoplain--Ogilvie. 29. such types as Pinusponderosa (var. scapulorum), Quercus undulata, and various shrubs of the oak and holly families. Associated with these are the cactus-like types, Opuntia, Cereus and Yucca. The vegetation is thus, for an arid re- gion, a considerable one. The surrounding plains present a marked contract; Opuntia, Cereus and Yucca, together with Artemisia (sage brush) form the prevailing types. The largest trees there are pinon and a small cedar. The result of this difference in climate is that the moun- tain springs give rise to streams which disappear entirely a short distance from their source. Within the Ortiz area there is no permanent stream which finds its way to the sea. For the greater part of the year the arroyos are en- tirely dry, and many of the springs dry up also. But when rain comes, it comes in quantities, and a few days of storm will start raging torrents. The details of the idea of the growth of river valleys and of cycles of erosion have been developed in regions of moderate climate and of equably distributed rainfall. It is evident that in such a region as the Ortiz the normal erosion cycle will be markedly different. Leaving aside for the ‘moment the larger question of the origin of the great plateaus, and also the special case of the Ortiz mountains, let us consider the theoretical erosion history of an ideal laccolith. : If we imagine a symmetrical laccolith of homogeneous rock, to have arched up the strata of previously horizontal rocks, the initial stage of erosion may be compared to that of Prof. Salisbury’s homogeneous, symmetrical island. But with this difference that in the case of the island the limit in down-cutting is a result of checked velocity and is at sea level; in the case of the laccolith the limit is formed by the point at which the streams disappear, and may be at any altitude. The transporting power of a Stream depends upon volume and velocity. An increase in volume increases the transporting power by more than a simple ratio; velocity depends upon volume and declivity; hence an increase in volume indirectly adds to the transporting power by in- creasing the velocity. And an increase in declivity aids the 30 The American Geologist. Sule transporting power by more than a- simple ratio. These facts were brought out thirty years ago by Gilbert in his classic memoir on the Henry mountains. The amount of corrasion which a stream can perform depends upon its load. The transported detritus forms the tool with which it cuts, but an excess of material prevents corrasion. When a stream has all the load it can carry, the entire energy is used in transportation, and there is none for corrasion. If there is an excess of detritus, the trans- porting power is insufficient and deposition takes _ place. When a stream empties into a body of standing water its velocity is checked, material is deposited and further corra- sion is impossible. The ordinary peneplain, of Powell’s type, is produced as a result of checked velocity. On emptying into the sea a stream’s velocity diminishes, it deposits material, and its valley widens by weathering. When several valleys widen at the expense of the interstream areas a flat is formed, and this gradually extends upstream, until a peneplain is pro- duced. But the initial cause of these results is checked velocity and that alone. The energy of a stream depends not only upon velocity but also upon volume. Obviously a decrease in volume would also lead to deposition and to a cessation of corra- sion. Such a decrease in volume might take place in vari- ous ways; but the common way in the plateau region is when‘a stream in its course passes from a less arid to a more arid climate. In the case of our ideal laecolith the rain would all be caught near the summit, streams would become established which would flow down the slopes, and on reaching the arid surrounding plain these streams would speedily dry up. This result would be accomplished partly by evaporation and partly by soaking in, as a result of the lower ground water level. In the case of the laccolith, the process is aided by lessened declivity. The form being a constructional one, puShed up out of a previously existing plain, there would be a change in grade in passing away from the slopes of the mountains. This decrease in declivity would produce a corresponding decrease in velocity. Hence lessened volume The High Altitude Conoplain---Ogilvie. a and lessened velocity would work together to produce depo- sition at a point near the edge of the disturbed area. If the rainfall were equably distributed the point of dis- appearance of streams would gradually move nearer the mountains as more material accumulated. The theoretical end of the cycle would come when the laccolith became so far reduced that it could no longer catch the moisture, and wind alone would carve its surface. This old age laccolith would in a general way resemble the mature island; it would have slight elevation, be carved by radial valleys, and would be surrounded by a cut plain sloping gently away on all sides, this in turn being surrounded by a built plain. The whole would be closely analogous to the sea level forms of peneplain grading seaward into stratified deposits. 3ut in the region under consideration this ideal cycle probably never took place, since it would normally be inter- fered with by the two factors, unequal annual distribution of rainfall and wind. The effect of the unequal distribution of rainfall is an- alogous to that of an oscillating coast. Given a coast that is alternately rising and sinking, no peneplain will be pro- duced. If an approximation towards it develops, a slight uplift will rejuvenate the streams causing them to incise steep-sided channels; a slight sinking will drown the streams and fill their channels with deposits. Similar processes are normally going on in the degrada- tion of a laccolith. The burning heat of summer pushes the point of disappearance nearer the mountains, and even most of the springs go dry. At some uncertain period in the fall or winter, rains come and then torrents rush down rapidly cutting through the previously formed alluvial de- posits, redepositing them farther out on the plain. These mountain torrents often change their courses entirely from One season to the next, the course depending upon the more or less fortuitous arrangement of the surrounding alluvial material. Therefore the surrounding conoplain is deeply scarred with arroyos and there are more arroyos than are ever full at any one time. Hence in no stage of the actual erosion cycle is the conoplain absolutely flat. In all stages it will be cut by gullies, but surface inequalities will be largely obliterated by filling with alluvial deposits. 32 The American Geologist. July, 1905 In the usual erosion cycle in a moist climate, deposi- tion is a mark of increasing age. ‘There are notable excep- tions, but in the typical, normal case a flood-plain is formed after a considerable amount of down-cutting has been done at the mouth of the stream. In the laccolithic cycle deposi- tion takes place at all stages and in all places except the uppermost slopes.. For if, after a rain, a flood stream ex- - tends its course two miles onto the plain and there dries up, for the last mile and a half or so it will have been losing volume and velocity and will have been depositing its material either as a flood plain or as an alluvial fan. If a few days later it has shrunk in volume and extends only one mile onto the plain, its transporting power will have decreased throughout its length and deposition will be tak- ing place at the edge of or within the mountains. As the stream continues to shrink, its transporting power decreases until material is dropped well within the mountains. This deposition of material is a normal feature of all stages of the erosion cycle, though obviously more material will have been deposited when old age is reached than in youth. The form taken by the alluvial deposits is somewhat different in the two climates. The general process of cut and fill is the same for both, but the surface configuration differs. An old valley emptying into the sea develops flood plains along its lower course and also a delta at its mouth. These deposits are laid down in standing or in slowly mov- ing water. The banks of the river are still higher than its chan- nel and the flood plain is a sort of filling dropped into the bottom of a curve concave upwards. The laccolithic de- posits are as a rule built up on a flat with no pre-existing valley, and they take the form ef alluvial fans. The con- fluence of several fans from neighboring streams may produce a plain. In the normal erosion cycle in a humid region the cross section of the valleys changes from a steep sided V in vouth, to a gentler sloped U in maturity. In arid regions the U shape never comes. If the valleys widen, it is by the retreat of nearly vertical cliffs. The reason seems to be that moisture and its results, soil and vegetation, are at The High Altitude Conoplain --Ogilvie. 33 a minimum, hence there are no causes to produce the soften- ing prominent in an eastern landscape. And when water is present at all, it comes in sufficient bulk to produce a tor- rent of large volume and high velocity. Such a torrent anywhere would cut steep-sided canyons, provided only that the rock cut into is sufficiently hard to stand in cliffs. In many cases joints are present which cause the rock to break off in blocks leaving cliff faces. So in the erosion cycle of our laccolith, the plain will not only be scarred at all stages, but it will at all stages be cut by steep-sided canyons. Another interference with the ideal cycle is the wind. No one who has seen the whirlwinds moving over the deserts of Sonora or Chihuahua can feel any doubt as to the great possibilities of wind as an erosive agent. The general effect of wind-upon a region such as the one under consideration would be the removal of fine material, thereby lowering the plains, the scarring of the hard rock by mechanical abrasion, and the drying of the soil. Such may be considered the normal factors of erosion, but the cycle in nature is usually interrupted, or has ab- normal conditions at the start. Among the interruptions may be mentioned vulcanism, the presence of some large river flowing to the sea, and climatic changes. For if some river is near enough to be reached by the streams, the lac- colith at once becomes a part of the drainage basin of that river and its cycle is limited by the level of the river, which in turn is limited by sea level. Variations in humidity would change the position of the point of disappearance, and damper epochs would produce rejuvenation. The actual laccolith is rarely ideal, but usually consists of several different intrusions, not necessarily circular in outline, into strata not originally horizontal, the whole more or less disturbed by faulting. The Ortiz mountains are abnormal in all these respects. It is no part of the present paper to describe them, but only to point out the generali- ties of this process as exemplified in them. If it is possible for a plain to be cut at high altitude in the case of a small and isolated laccolith, the question at once arises as to whether some similar process may not 34 The American Geologist. July, 1906 have produced the broad areas of the great plateaus. It is difficult of demonstration, but the impression is very strong that these plains are not peneplains cut at sea level, but that they were produced at their present altitude by some process more or less analogous to the preceding. Whatever the factors affecting the region as a whole, there seems no manner of doubt that the conoplain of the Ortiz has been produced in some such manner. There is no evidence whatever of the presence of any large lake or sea that could have afforded even a temporary baselevel for the cutting. Nor is there any evidence that the country has been reduced to a lower level than it has at present, since the Miocene. We are forced to the conclusion that the sloping plains surrounding mountain masses were cut at their present altitude, and that diminishing volume was the essential factor in the cutting. GENETIC AND STRUCTURAL RELATIONS OF THE IGNEOUS ROCKS OF THE LOWER NEPONSET VALLEY, MASSACHUSETTS.* By W. O. CROSBY, Boston, Mass. INTRODUCTION. The Lower Neponset valley, or more specifically, that part of the valley of the Neponset river within the limits of the Boston basin, properly embraces all that part of the Boston basin between the Blue hills, a denuded anticlinal axis dividing the Boston basin from the parallel and over- lapping trcugh of Carboniferous sediments known as the Norfolk basin, and the broad band of conglomerate extend- ing westward from Savin hill on Dorchester bay through Dorchester, Roxbury, West Roxbury, Brookline and New- ton into Wellesley and Needham. This great belt of con- * This paper is an advance presentation, in outline, of a portion of Part iv of the author’s detailed and systematic study of the Geology of the Boston Basin in course of publication in the series of Occasional Papers of the Boston Society of Natural History. For the petrographic distinctions in this field the author is indebted to Dr. Florence Bascom, whose preliminary observations on the volcanics only have been pub- lished (Bull. Geol. Soe. Ameriea. vol. 11, 115-126), and whose more com- plete and elaborate work on both the voleanics and plutoniecs awaits publication in connection with the forthcoming Part iv of the Boston Basin series. Relations of the Igneous Rocks—Crosby. 35 glomerate, some three miles in normal breadth, is, struc- turally, one simple, flat-topped and somewhat unsymmet- rical anticline, the central and dominant arch of the Boston basin (the Shawmut anticline), separated from the Blue hills or southern highlands by the Lower Neponset valley, and from the northern highlands by the Lower Charles valley, each of these main lateral valleys exhibiting, in the general view, a synclinal structure, with slate as the pre- vailing surface formation, but being, withal, as complex in geological structure as the central ridge or water-parting is simple. As thus defined, the Lower Neponset valley is, west of Boston harbor, a rectangular area some three miles wide and eight to ten miles long, including, on the mainland, small portions of the towns of Canton and Dedham, the whole of Hyde Park, the northern half of Mil- ton and Quincy and the southern half of West Roxbury and Dorchester. It is an area of great topographic as well as geologic complexity, and although, in general, low lying, includes, in Bellevue hill, the highest land within the Bos- ton basin. The district here included in the Neponset valley is not now wholly drained by the Neponset river, this study naturally following geologic, more closely than topographic or hyprographic, boundaries. The Lower Neponset valley is essentially an epitome of the entire basin, since it also consists of a central anti- cline of conglomerate bordered on either side by a well- defined slate syncline. The southern syncline, extending through Milton and Quincy, widens rapidly eastward, a somewhat open and composite trough, while the northern syncline, extending through West Roxbury and_ Dor- chester, is a relatively deep and narrow isocline. The immediate valley of the Neponset is developed in the complex and strongly denuded anticline which thus divides the more southerly of the two main troughs of the Boston basin, and which narrows eastward for the simple reason that the axis pitches or inclines in that direction. The prevailing sedimentary rock of this belt is conglom- erate, and the attitude or structure of the conglomerate as a whole is anticlinal. It dips northward along the north- ern border, passing beneath the slate of the deep and nar- 36 The American Geologist. July, 1905 row Dorchester-West Roxbury syncline; while along the southern border the dip is southerly and the conglomerate passes below the slate of the much broader and composite Quincy-Milton syncline. That the anticline itself is not a simple arch is plainly indicated by the narrow band of slate developed at intervals along the middle of the conglomerate belt and the existence of at least two anticlinal axes, pitch- ing to the east and rising to the west, is further indicated by the fact that toward the west, where erosion has cut through the conglomerate and interbedded flows of basic lava we have exposed, not one, but two, ridges of the under- lying crystalline rocks—granite and felsite—representing the floor upon which the conglomerate series was deposited. These two axes are, at most points, of unequal prominence; and in their denuded western extensions the northern axis largely predominates , forming the broad, irregular and broken ridge projecting into the Boston basin from the western highlands of Dedham and Needham and including the granite, quartz porphyry and felsite of the Bellevue Hill district and the Stony Brook reservation, the felsites of the northern part of Hyde Park and the felsites and more basic lavas of the Mattapan district of Dorchester. The minor southern axis is seen in the narrow band of fel- site and basic lava, lying mainly south of the Neponset, between Readville and Milton Lower Mills. Over a part of this area several flows of basic lava or andesite are interstratified with the conglomerate; and during the geological revolution or period of disturbance following the accumulation of these strata and the formerly overlying slate upon the old floor of felsite and granite, they were forced into a gigantic arch from one to nearly three miles broad. This great fold, however, partially broke down in the making, and its collapse was attended by the forrmation of the minor folds and numerous faults. Subsequent erosion has been so extensive as to remove the entire thickness of slate from the crest of the great anti- cline, except where it has been carried down most deeply by these minor folds and the faults, occurring now in -nar- row and discontinuous belts wedged in between the larger masses of conglomerate. The erosion has also been suffi- Relations of the Igneous Rocks—Crosby. 37 cient to cut through the conglomerate series and the inter- bedded andesite, toward the western end of the arch, where they were most elevated, and thus expose the ancient foun- dation of felsite and granite. Probably no phase of this study possesses a greater in- trinsic interest than the comparison of the denuded major axis of the Neponset anticline with the Blue Hills complex, which is but the denuded axis of the great anticline separ- ating the Boston and Norfolk basins; and aside from the disparity in area, it is surprising to find how fnarked is the similarity, except in minor details, and how few are the vital contrasts. In general terms, it may be stated that hardly anything is precisely similar in the two areas and nothing is radically different. In the smaller area as in the larger we have isolated masses of Cambrian strata involved in a complex of post-Cambrian granitic rocks, including the normal granite, the contact zone of fine granite and quartz porphyry, the effusive felsites and the intersecting dikes of diabase of several different systems. The chief contrast is found in the relatively greater abundance in the Neponset complex of the effusive felsites, their more varied character, the great profusion of dikes of felsite in the granites, the more positive identification of some of the principal vents or points of emission of these acid lavas, and the far more complete and clearer exhibition of their relations to the later basic lavas and the inclosing Carboniferous strata. Among the problems of special interest presented by the Neponset anticline and, apparently, admitting of suc- cessful determination, may be mentioned: the detailed rela- tions of the rocks of the basal complex; the mutual rela- tions of the acid and basic lavas—rhyolite (felsite) and andesite; and the relations of both types of volcanics to the THE BASAL COMPLEX. The basal complex may best be defined as comprising all of the pre-Carboniferous terranes of this region, both sedimentary and eruptive; or more specifically, as consist- ing of the Cambrian strata and any other pre-Carboniferous and pregranitic sediments which future investigation may prove to exist here, together with the intersecting and associated igneous rocks of pre-Carboniferous age, includ- \ 38 The American Geologist ciety aes ing the normal granite or main body of the batholite, and its contact zones of diorite, fine granite and quartz por- phyry, and the dikes, necks and flows of acid lavas or fel- sites. As thus defined, the igneous part of the complex is clearly the product of the chemical and textural differenti- ation of a single great body of magma, embracing, besides the truly plutonic mass or batholite proper, developed, with its variable contact zone, under and in the Cambrian strata, the intrusive and effusive masses evolved, after extensive erosion of the Cambrian cover, from either still unsolidified or remelted deep-seated portions of the batholite. That the batholite, with the complicating sedimentary and igneous phases, which gives it the character of a true and typical complex, is continuous under all the newer formations of the region and, in its successive phases, essen- tially contemporaneous throughout, is highly probable; and the variations observed from point to point must, there- fore, be regarded either, as actual and due in part to differ- ences in the original magma resulting from the fusion of the pre-Cambrian floor and in large part, also, to the vary- ing thickness and composition of the original Cambrian cover, or as merely apparent and due to the varying depths of pre-Carboniferous and post-Carboniferous erosion, or again, as due to the localization of the intrusive and effusive phenomena which followed the formation of the batholite proper, adding greatly to its structural complexity. If, with these ideas in mind, we compare more partic- ularly than heretofore the portion of the basal complex rising westward from beneath the Carboniferous sediments of the Neponset valley with the portion exposed, as the result of still more extensive erosion, in the Blue Hills»area, we find the more notable differences to be as follows: First, the normal granite of the Neponset valley is prevailingly coarser grained and the ferromagnesian constituent (chiefly hornblende) is more generally and extensively altered (chloritized). Second, the differentiation of the contact zone appears to have been almost wholly textural, and not, to any important extent, chemical, in the Neponset Valley district; and hence we find here only traces of diorite (which is also true of the Blue hills) and nothing closely Relations of the Igneous Rocks—Crosby. 39 corresponding to the basic porphyry and the basic phase of the fine granite of the Blue Hills area. Third, the effusive acid lavas or felsites are, relatively, more abundant and far more varied in the Neponset valley than in the Blue hills. Fourth, the dikes of both acid and basic lavas so characteristic of the basal complex in the Neponset valley are practically or wholly wanting in the Blue hills. Fifth, the necks or actual vents of the effusive acid lavas are far more normally and typically developed in the Neponset valley than in the Blue hills, while the vents of the basic lavas are wholly wanting in the latter area. Sixth, the dikes of diabase, which are found in the eastern and north- ern parts, and are practically wanting in the main range of the Blue hills, are, in the Neponset valley, characteristic of all parts of the complex as well as of the overlying sedi- ments, no considerable area being free from them. Seventh, erosion has left in the Neponset Valley section of the com- plex, so far as itis now exposed, only very scanty traces of the original Cambrian cover. GENERAL HISTORY OF THE COMPLEX. After what precedes a brief statement will suffice here, the main purpose being a more systematic outline, pref- atory to the lithologic and structural details of the com- plex. As in the Blue Hills area, this area or part of the general batholite of eastern Massachusetts is believed to have been developed beneath a great thickness of Cambrian, and possibly of later, sediments, of which erosion has left only a few highly altered remnants. The thickness of the Cambrian cover was due primarily to extensive sedimenta- tion and secondarily and chiefly to severe or isoclinal plica- tion. The thickening of the super-crust thus determined was sufficient to induce a rise of the isogeotherms, an out- flow of the subterranean heat, so marked as to involve soft- ening and final fusion of the sub-crust or floor on which - the Cambrian sediments were deposited, developing thus a great body of granitic magma, the corrosive action of which led to the absorption of considerable volumes of the sedi- mentary cover and gave rise, no doubt, to the normally * highly irregular and unconformable contact. This thickening of the super-crust and consequent great 40 The American Geologist. July, 1905 heat invasion was, doubtless, accompanied by a strong ele- vation of the surface, permitting extensive erosion, which, in turn, favored the refrigeration of the batholite and the development from the originally homogeneous magma of a _ vast body of normal granite, with a contact zone consisting, normally, of an inner layer of fine granite and an outer layer of quartz porphyry, both phases of the contact zone being the products mainly of a textural rather than a chem- ical differentiation of the magma. Long continued erosion, removing in large part the sedimentary cover of the batholite and probably cutting at some points through its contact zone into the normal gran- ite, was followed by a period of volcanic activity, due pos- sibly to cracking and hydration of the body of the batholite, during which, acid lava, chiefly rhyolite, now existing in a devitrified form as aporhyolite or felsite, was poured out over the eroded surface of the batholite. Several of the volcanic necks or vents of these effusive eruptions have been definitely located and their details of form and struc- ture more or less fully worked out. From the vents or chimneys of these most ancient volcanoes of the Boston basin radial dikes of felsite extend outward into the granitic rocks. As a chronologically distinct record, the complex was now complete; but it was destined to be still further complicated; for these effusive acid eruptions appear to have marked the beginning of the progressive subsidence which inaugurated the deposition’of the Carboniferous sediments, beginning with the great conglomerate series; and during the subsidence and clastic sedimentation the effusive eruptions continued, but became of more basic character—grading from rhyolite through trachyte to an- desite, which in its present altered form as apoandesite or porphyrite has been heretofore classed as melaphyre, but “is now known to be less basic than that type. The ande- sitic eruptions, from, presumably, greater depths than the source of the acid lavas, are marked by fissurelike necks, by numerous dikes cutting all the older rocks, and espec- ially by successive massive flows or contemporaneous beds intercalated in the conglomerate series. The volcanic activity finally ceased and continued sub- Relations of the Igneous Rocks—Crosby. 4I sidence introduced the deep water conditions permitting the deposition of the slate series into which the conglomerate series gradually merges upward. The deposition of the slate series was closed, it is supposed, by the Appalachian revolution, during which the Carboniferous sediments were strongly folded and faulted and injected by still more basic magma from, possibly, still greater depths, forming the older or east-west series of diabase dikes, now largely chlo- ritized or typical greenstone. Still later, and probably con- temporaneously with the Triassic sedimentation and ac- companying igneous activity in the Connecticut valley, were formed the diabase dikes of the newer or north-south series. With this the rock formations of the Neponset valley were complete, and its later geological history is recorded only in the erosion accomplished during later Mesozoic and Tertiary ages and culminating in the Bes ice invasion of post-Tertiary or Pleistocene time. THE CAMBRIAN STRATA. The existing small remnants, the larger less than a thousand feet long, of the body of Cambrian strata which we suppose to have once formed a continuous cover over the batholite in the Neponset valley, as in other parts of the Boston basin, appear to be confined to the vicinity of the Boston and Hyde Park boundary, in the eastern part of the Stony Brook reservation and the immediately contiguous territory. The sedimentary rock, of supposed Cambrian age, is all slate, of a uniformly massive, hard and distinctly meta- morphic character. The prevailing color is dark gray; but it varies to lighter shades; and very generally the rock is perceptibly veined or clouded with the green of epidote, indicating that the slate was, originally, more or less cal- careous, the lime having as an essential phase of the igne- ous matamorphism, combined with the alumina and silica of the slate to form epidote. This feature allies it with the Lower Cambrian slates of Weymouth, Quincy, Nahant, etc.; but in other respects it bears a striking resemblance to the massive, gray, non-caleareous Middle Cambrian slates, as these are developed on Hayward creek in Braintree and 42 The American Geologist. duly) tae along the north side of the Blue hills. It exhibits in a good degree the characters of a true hornstone; but it is no- where of flinty hardness; and the fact that it is never visibly micaceous testifies to the essentially non-alkaline character of the sediment. As a rule, the stratification is hopelessly obscure; but at a few points, which are so distributed as to cover practically the entire group of ledges, it is fairly dis- tinct and entirely unequivocal. The attitude of the bed- ding is, as usual in the Cambrian of the Boston basin, very constant, with east-west strike and vertical dip. The essential relation of these sediments to the com- plex is clearly indicated, not alone by their metamorphic character, but also by typical igneous contacts with the fine granite and quartz porphyry of the contact zone, and irregular dikes or apophyses of the quartz porphyry and more regular dikes of normal felsite. BODY OF THE BATHOLITE. - Normal Granite —This is a coarsely crystalline aggre- gate of feldspar and quartz, chiefly, with a small propor- tion of a dark constituent regarded by Dr. Bascom as chlo- ritized amphibole. ‘The feldspars, according to this author- ity, include orthoclase, commonly of a pinkish tint due to oxidation, and a lime-bearing albite in which the greenish tint due to epidotization is more or less marked. The an- alysis shows an acid rock, similar to the normal granite of the Blue hills, but rather more basic and richer in plagio- clase, though poorer in the ferro-magnesian constituent. The outcrops of normal granite are chiefly confined to two rather irregular areas; and the general relations of these to the complex is not central, as might seem most natural, but peripheral.” They form; - “respectively, =the northern and southwestern borders of the complex, and converge but, apparently, do not meet, to the northwest- ward, in the vicinity of Grove and Center streets. The dis- positions of the normal granite is such as to suggest at once a general monoclinal or shallow synclinal structure for the complex,—the surface of the normal granite forming a trough the axis of which pitches to the southeast, thus allowing the normal granite to slope southward and north- eatsward beneath the contact zone of fine granite and Relations of the Igneous Rocks—Crosby. 43 quartz porphyry and a great thickness of volcanic and sedi- mentary formations. In the direction of its disappearance the normal granite does not reappear north of the Blue hills; and undoubtedly its disposition, especially in relation to the unaltered sedimentary formations which meet it ab- ruptly on the north, in the West Roxbury district, finds its. readiest explanation in a profound displacement along the northern border of the complex, with the downthrow, of course, to the north. The normal granite is observed at many points to grade upward into the fine granite by which it is bordered; and its surface continuity is frequently interrupted by island-like outliers of the fine granite. These relations are particularly well-exhibited in the broad and massive ledges in the-area bounded by Washington, Grove and Center streets and Cottage avenue; and nowhere more favorably than in the vicinity of the large quarry on Cottage avenue,. northwest of Washington street. CONTACT ZONE OF THE BATHOLITE. Fine Granite—The chief difference between this type and the normal granite is textural. The essential minerals, according to Dr. Bascom, are the same, with the addition of a little microcline and oligoclase to the _ feldspars. Quartz is reported as more abundant, and the chloritized ferromagnesian constituent as less so, and these distinctions are confirmed by the analysis, which shows higher silica and lower lime, magnesia and iron. The fine granite belongs to the contact zone and hence overlies the normal granite. It might, therefore, where not removed by erosion, be expected to exhibit a broad areal development, but for the fact that it is, in turn, cov- ered by the quartz porphyry phase of the contact zone. In harmony with this general relation and the shallow syn- clinal structure of this part of the batholite, the principal area of the fine granite takes the form of an irregular V- shaped belt, 1000 to 3000 feet wide, separating the normal granite on the north and southwest, from the quartz por- phyry on the south and northeast, respectively. As to the thickness of the fine granite, we have no very definite clue. | No approximately vertical or continuous 44 The American Geologist. Jala section shows both the normal granite below the fine granite ‘and the quartz porphyry above it. In other words, we have no data for a direct determination of the thickness, save that it must exceed the hight of the highest hill com- posed wholly of the fine granite, or say 75 feet. It would be readily deducible from the surface breadth if the dip were known. Assuming the dip to be low and inversely proportional to the surface breadth, gives a maximum thick- ness of a few hundred feet at the most; and 100 to 200 feet may, perhaps, be accepted as a conservative estimate, con- firming the conclusions reached in the study of the Blue Hills complex. The finer granite of the contact zone is, in a fair sense, a bed of passage, since it grades downward into the nor- mal granite and upward into the quartz porphyry; and, normally, its original contacts are nowhere sharply de- fined, but distinctly blending. It may be noted, however, that, as in the Blue Hills complex, the contact with the normal granite, though blending, is rather abrupt, the com-_ plete transition from the one rock to the other being ac- passage upward into the quartz porphyry is usually more or, possibly, in extreme cases, a single foot. Although the complished in some exposures in the breadth of a few feet sedimentary rocks. gradual, all observers must recognize that the fine granite, so far from being all gradation, is chiefly remarkable for the uniformity of texture throughout almost its entire thick- ness. In fact, it rivals the normal granite in this respect. Locally, and especially near the quartz porphyry, it may pass into a true microgranite; but it is in general a macro- granite of very homogeneous aspect.* That the fine granite is older than the normal granite and younger than the quartz porphyry, and that these three distinct but blend- ing sedentary zones of the batholite exhibit the structural relations which this sequence requires, will probably not be questioned by those familiar with the field evidence. * The explanations of the homogeneity of the fine granite and its abrupt yet blending passage into th2 normal granite suggested in Part Ill. of the Boston Basin Geology (Occas. Papers, Boston Soc. Nat. History, iv, 354 et seq.) are still regarded as valid, and as applicable in this new field. _ Relations of the lgenous Rocks—Crosby. 45, Quartz Porphyry—This upper or peripheral member of the contact zone has been designated by Dr. Bascom the rhyolitic facies of the granite or more succinctly rhyolite, and more explicitly porphyritic aporhyolite; and for this usage the petrographic characters undoubtedly afford ample warrant. But in order the more sharply to distin- guish this essentially plutonic type from the much younger and very dissimilar intrusive and effusive rhyolites, it is proposed to employ here the good descriptive term quartz porphyry. The rock in question is in every instance a true quartz porphyry, with conspicuous phenocrysts of both quartz and feldspar; and, as befits its plutonic origin, it is of remarkably uniform character, matching the granites in this respect; while the clastic, fluidal and spherulitic struc- tures so characteristic of the newer rhyolites are conspic- uous by their absence. Such variation as the quartz por- phyry shows is due chiefly to its gradation downward into the fine granite; and, as Dr. Bascom has noted, its texture, though aphanitic, allies it with the microgranitic phase of the fine granite, and unlike the younger rhyolites it is rarely truly cryptocrystalline. In its distribution the quartz porphyry tends to form a V-shaped zone concentric with the fine granite, and sepa- rating the underlying fine granite from the overlying effusive rhyolite or felsite. The lower border of the quartz porphyry is rendered rather vague and indefinite at most points by its blending contact with the fine granite. The upper border, on the other hand, where the quartz por- phyry meets the effusive rhyolites or felsites is, in the na- ture of the case, sufficiently definite but highly irregular, since we have here a true erosion unconformity, and two formations, although of closely similar composition and probably derived from the same original magma, are strong- ly contrasted in structure and widely separated in geolo- gical time. Summary and Comparison—Neglecting unimportant occurrences of diorite and aplite, which may be described, respectively, as relatively basic and relatively acid phases or segregations of the normal granite, and hence as pro- ducts of a chemical differentiation of the main body or 46 The American Geologist. tae primal magma of the batholite, we have now considered all of the sedentary or truly plutonic rocks of the batholite. These have been described in the order of superposition, which is, of course, the inverse order of age, since the re- frigeration of the batholite must have progressed from the periphery downward or centripetally.- That the differenti- ation of the normal granite and the contact zone, and the further differentiation of the fine granite and quartz por- phyry of the contact zone, are not wholly textural is, as noted by Dr. Bascom, clearly shown by analyses, according to which the normal granite is the most basic and the fine granite the most acid, while the quartz porphyry is inter- mediate in composition, although not so in position. By way of explanation of this chemical relation, Dr. Bascom has suggested that specific gravity and convective currents may have been factors in producing a somewhat more acid peripheral zone to the batholite, while the outer or quartz porphyry border to this zone, following the general law of the order of crystallization (virtually fractional crystalli- zation), by its earlier crystallization left the inner portion of the zone or fine granite more acid than either the quartz porphyry or normal granite. To this explanation may, perhaps, be added the influence of hydration. It appears reasonable to suppose that the primal magma of the batho- lite, formed under a thick and, necessarily, a hydrated sedi- mentary cover, and due in part to the absorption of large volumes of this cover, would naturally be more highly hydrated in its superficial than in its deep-seated portions ; and since the characteristic elements of an acid magma, in- cluding silica and the alkalies, have a stronger affinity for water than have the lime, magnesia and iron oxide charac- teristic of basic magmas, we have here a cause tending to keep, if not to make, the batholite superficially acid. That, in comparison with the granitic rocks of other districts, this part of the batholite “was formed under a moderate depth of cover, is believed to be indicated by the relatively slight amount of chemical differentiation, by the absence of an original micaceous constituent, and especially by the almost entire absence of a pegmatitic phase im the normal granite. The absence of marked differentiation ex- » Relations of the Igenous Rocks—Crosby. 47 tends, in the main, to the earlier intrusions in the batholite, since, with one exception, these are relatively acid, and differ but little in composition from the sedentary members of the batholite. (Continued in August Number.) EDITORIAL COMMENT. ANOTHER METEORITE IN THE SUPREME COURT. It was decided by the lowa supreme court, in the case of the Winnebago meteorite, that the meteorite belongs to the owner of the land on which it falls. The tenant found the stone and sold it. The owner brought suit to regain it, and after some years of litigation and delay the court assigned the meteorite to the owner of the land. The Oregon meteorite case is somewhat different. A metallic mass is admitted by both parties to be of meteoric nature and origin, and as such, according to the lowa de- cision, it belongs to the owner of the land on which it fell. The date of its fall however is unknown, and there is evi- dence tending to show that it was a piece of personal prop- erty, separate from the land on which it was found, for many years prior to the date of discovery. The issue and the attendant conditions have been stated as follows by the Oregon Journal: The Oregon City meteorite case was argued before the supreme court yesterday. This is an action brought by the Oregon Iron & Steel company to obtain possession of the metallic meteorite found by Ellis Hughes in November, 1902, on the land of the Oregon Iron & Steel company, about two and a half miles west of Oregon City. The interesting subject of this centroversy was found standing up- right on a slight knoll. It is of metallic composition, with a dull, rusty surface, its top or flat surface being gouged out into huge pot- holes or washbowls. As it stood it resembled very much in ap- pearance a mammoth mushroom or inverted bell, in size seven by ten feet across at the top, and four and a half feet thick, its weight being estimated at from three to four tons. It has the specific gravity of soft iron, and in composition is 90 per cent soft iron, 10 per cent nickel, with a trace of cobalt. Hughes alleged that this was an abandoned Indian relic and 48 The American Geologist. July, 1905 that he was the first white discoverer of it and, believing he had a right to it, he constructed a rude wagon and hauled it to his own home, about three-quarters ef a mile distant. He alleged that this meteorite was the property of the Clackamas tribe of Indians (now disbanded and nearly all dead), and that they had a tradition that this magic rock, called by them ‘‘Tomanowos,”’ came from the mocn, and possessed supernatural influence. He claimed that it was fashioned, erected, maintained and used by them to hold the fluid in which they were wont to dip their arrows before engaging in battle with their Indian foes, and that their young warriors were compelied to journey over there and visit this spirit being on the darkest nights. To substantiate these claims two Indian witnesses were produced, who testified that the above facts were true, according to the legends of their tribes. One of them was a mem- ber of the Klickitat tribe of Indians and the other was a Wasc Indian. Goth parties to this case agree that the object is a meteorite, but no proof has been offered by either to show when it arrived on earth. The Oregon Iron & Steel company denies that it is an Indian relic, and claims title to it by virtue of ownership of the land upon which it was found. It may safely be assumed, probably, that this iron fell on the land where it was found, although there is no proof of it. The Indians who previously visited and worshipped it could not have transported it. If they had ownership of the land they owned the specimen. As they did not remove it, when the land passed from them it would seem that the meteorite went with the land. But the consideration that they had used it as a special object, for a special purpose, foreign to the uses to which land as such is devoted seems to make it an object of personal property. They may have erected it in the position in which it stood, and may have deepened the “potholes” on its upper surface. If a man sculptures a statue from some rock on his land, when he sells the land the statue does not go with the land. If the Clackamas Indians did not own the land, and yet visited and controlled the specimen for a specific use without ob- jection from others, it seems reasonable to assume that the specimen was not an appurtenance of the land and that they had the right to remove it. If they abandoned it, without removal, it seems to belong to that class of Indian relics of which many examples are known and which the finder, rightly or wrongly, becomes the owner. If the specimen is an Indian relic the ownership thereof Review ot Recent Geological Literature. 49 may still be in the owner of the land. He is a trespasser who wilfully passes on to his neighbor’s domain; and he is still more a trespasser if he removes, against the owner’s protest, any of the property of his neighbor. N. H. W. Note.—Since the foregoing was written the Oregon supreme court has decided this case, as follows, as published in the Portland Oregonian: Oregon Iron and Steel Company, respondent, vs. Ellis Hughes, appellant, from Clackamas county, T. A. McBride, judge; affirmed; opinion by Chief Justice Wolverton. Held, that a meteoric rock is a part of the real property upon which it falls, and evidence that Indians worshipped the rock and dipped their arrows in the water held in its cavities is not suf- ficient to show that the Indians had dug the rock from the ground and acquired title to it as personal property. The question whether Indian ownership and abandonment is sufficient ground upon which to predicate title in the finder is not decided. The court did not consider the evidence as to the ownership of the specimen as personal property by the Indians of sufficient force to warrant the reference of the case to a jury for determination. That evidence failing, there was left the bare question as to whether the meteorite belonged to the real estate or to the finder. In that the Oregon court coincided with the Iowa court 7 re Winne- bago meteorite. N. H. W. REVIEW OF RECENT GEOLOGICAL LITERATURE, Contributions to Devonian Paleontology, 1903. Henry Shaler Wil- liams and Edward M. Kindle. Bull. U. S. Geol. Surv., No. 244, 1905, pp. 1-144. — Bearing of Some New Paleontologic Facts on Nomenclature and Classification of Sedimentary Formations. Henry Shaler Wil- liams, Bull. Geol. Soc. Amer., Vol. 16, March, 1905, pp. 137-150. Bulletin No. 244 consists of two parts, No. I. listing and dis- cussing “Fossil faunas of the Devonian and Mississippian (Lower Carboniferous) of Virginia, West Virginia and Kentucky,” while part II. considers in a similar manner the “Fossil faunas of Devon- ian sections in central and northern Pennsylvania.” A large num- ber of sections in Kentucky, Virginia and West Virginia are 50 The American Geologist. July, 1905 described by Dr. Kindle and accompanied by lists of fossils of the various faunules. The above is followed by a series of short articles, among which may be mentioned “Correlations,” ‘“‘The Rens- selaeria fauna,” “‘The black shale and its fauna,’ “The upper De- vonian faunas of the middle Appalachians” and a “List of diagnostic Chemung species” by professor Williams. In part II. the descrip- tions of the sections in central and northern Pennsylvania are mainly by Dr. Kindle; but the formational and faunal correlation is considered much more fully than in the preceding part by both Kindle and Williams. ; These two papers have recently been reviewed by professor Schuchert* who considered critically the lower Devonian, or the Helderbergian and Oriskanian series. It appears that similar notes concerning the middle and upper Devonian, to which this review will be largely restricted, might be of value. Professor Schuchert seems inclined to question the identification of Anoplotheca acutiplicata from the black shale near Covington ‘and Hot Springs, Virginia. The writer considers that the identi- fication is probably correct, for the same species occurs near the base of the black shale or Marcellus member of the Romney forma- tion in western Maryland. The Maryland specimens were exam- ined by Dr. John M. Clarke so that no question can be raised re- garding their specific identity. From the occurrence of the above species and Anoplia associated with others which are “regarded as confined to the Marcellus shale of New York” professor Williams concludes “that the black shale was deposited in a thick mass in the Appalachian trough before the fauna of the Onondaga (Corni- ferous) formation was extinct.” In connection with the above it is well to remember that the Onondaga fauna entered New York from the west and, generally, is supposed to have reached no farther south than northeastern Pennsylvania. Dr. Clarke has shown that “early Marcellus devosits in eastern New York were * *. * con- temporaneous with late Onondaga deposits in western New York.’+ On page 45 of the Bulletin professor Williams speaks of the Romney formation as though it were composed entirely of black shale and this idea is expressed by him more distinctly in the second paper under consideration. The term Romney formation was first published by Mr. Darton in 1892 in this journal and was applied to the rocks in the vicinity of Romney, a town scarcely 15 miles south of the Potomac river in Hampshire county in the north- ern part of West Virginia. It is located within the Potomac basin and there is very slight change in the lithology or fauna of the deposits in western Maryland to which this name has subsequently been applied. The writer has shown that both on lithological and faunal grounds the Romney formation of northern West Virginia and western Maryland may be divided into two members. The lower one is composed principally of fissile black shale, weathering * Am. Jour. Sci., 4tn Ser., Vol xix, June, 1905, pp. 460-463. +N. Y. State Museum, Bull. 25, 1905, p. 668. Review of Recent Geological Literature. 51 to a brownish or buff color, together with some bands of dark-colored thin limestone, with a total thickness of about 500 feet. The lime- stones contain Agoniatites expansus (Vanuxem) which is so char- acteristic of a thin limestone in the lower part of the Marcellus shale in New York that its generic name has been given to it, while the black shales contain numerous specimens of Liorhynchus limr- tare (Vanuxem) and some other species which are regarded as characteristic of the New York Marcellus shale. In a general way this member corresponds with the Marcellus shale of New York with which it has been correlated. The upper member is composed of bluish or bluish-gray shales and sandstones with an approximate thickness of 1,100 feet. This member contains numerous specimens of characteristic Hamilton species of New York and frequently the entire 16 species which professor Williams has previously listed as the “dominant species of the Hamilton formation of eastern New York and Pennsylvania.” Evidence indicates that the deposits of the Romney formation in Maryland apparently closed at about the same geological time as the Hamilton beds of New York, and in a general way this member has been correlated with the Hamilton beds of New York. It is not intended to state that the limits of the Romney formation in northern West Virginia and Maryland are exactly contemporaneous with the limits of the Erian series of New York; but there is a striking similarity in most details and it is believed that there is no serious error in this general correlation. The deposits, called Romney shale, which professor Williams has studied in the field, their fossils. in the laboratory, and _dis- cussed in Bulletin No. 244 are located in southern Virginia and eastern Kentucky. These collections later were supplemented by others made by Dr. Kindle in Kentucky, Virginia and southern West Virginia. It appears, however, that the locality farthest north from which collections were made is 110 miles or more to the southwest of Romney and, apparently, the nearest outcrops of the so-called Romney shale which professor Williams studied in the field are 220 miles or farther to the southwest of that town. It is well known that there is a rapid thinning and marked lithologic change in the Devonian deposits as they are followed from the Potomac basin to the southwest. Professor Williams’ own statement “that in the correlation of local formations the same species of fossils alone (when so much as 50 miles of distance separates their sta- tions) can not be relied on for establishing more than a general homotaxial relation of the formations compared’* would suggest caution in correlating with the Romney formation the deposits of Bland county in southwestern Virginia, 220 miles to the southwest. The statement of professor Williams that “the rocks belonging to the part of the column called Romney, in central and southern Vir- ginia, contain chiefly the faunas found in New York in the Mar- cellus, Genesee, and Nunda (‘Portage’) with only traces of the Ham- * Bul. Geol. Soc. Amer., vol. 16, p. 147. 52 The American Geologist. July, teen ilton fauna near their base’; is probably true for the region which he studied but is incorrect for the Potomac basin in which the typical outcrops of the Romney formation occur. As we have shown above, the Romney formation in its standard region contains in its lower member essentially the fauna of the Marcellus shale and in its upper member that of the Hamilton beds of New York. It is not until in the succeeding or Jennings formation that the Genesee, Naples or Portage, Ithaca and Chemung faunas are found. Probably that portion of part II. of most general interest is the discussion and correlation of sections in Northumberland and Columbia counties of central Pennsylvania which had been adopted as standard ones by the state survey in the interpretation of the geology of that part of the state. Perhaps the most important one is the Catawissa section on the Susquehanna river which was very carefully studied by Dr. Kindle in the field and the correlation re- viewed by professor Williams. Dr. Kindle shows that the calcar- eous shales in this section which were correlated with the Tully limestone by the Pennsylvania survey contain a Hamilton fauna, “not one of the characteristic Tully forms appearing.” Dr. Kindle, however, considered that the zone “occupies the _ stratigraphical position of the Tully limestone of New York” while professor Wil- liams stated that it and the two subjacent zones contain “the normal fauna of the Hamilton formation.” The writer showed in 1894 that the caleareous Shale in Pike and Monroe counties in northeastern Pennsylvania, which the state survey correlated with the Tully limestone of New York is succeeded by some 200 feet of very fossil- iferous shales containing a characteristic Hamilton fauna which he referred to the Hamilton formation.* The investigations of Dr. Kindle clearly show, however, that the calcareous shales of central Pennsylvania correlated with the Tully limestone of New York by the Pennsylvania Survey occur at a higher stratigraphic horizon than those of northeastern Pennsylvania as was inferred and pub- lished by the writer in 1894.4 The succeeding 225 feet of bluish- black shales are correlated, on account of lithological similarity, with the Genesee shale and rather more than 25 feet above their top appears the first faunule of the Nunda (Portage) formation. Professor Williams states that the name Nunda formation has been adopted to designate what has heretofore been called the Portage or Nunda group. Two hundred feet above the top of the Genesee shale is a faunule containing Spirifer pennatus var posterus which is considered as the first appearance of the Ithaca fauna that then continues through about 1,400 feet of deposits to almost the base of the lowest red shales. Dr. Kindle states that no characteristic Chemung forms appear in these deposits and professor Williams concludes that ‘“Faunally the evidence of the Chemung formation §Ibid, -p. 148. Bul. U. S. Geol. Surv., No. 120, »p., 71-73. PLbIG=) 2s toe Monthly Author's Catalogue. 53 must be looked for in the still higher strata.” The last deposits considered were correlated with the Chemung formation by the Pennsylvania survey in the upper portion of which they reported the characteristic Chemung species Spirifer disjinctus. From the lowest reported horizon of this species Dr. Kindle carefully searched every remaining foot of the so-called Chemung deposits without find- ing a single specimen of Spirifer disjunctus. This is in perfect harmony with the writer’s experience in northeastern Pennsylvania where he failed to find this species which was reported in rocks of so-called Chemung age.* This detailed work of Kindle and Wil- liams confirms the writer’s correlation in 1894 of the so-called Che- mung of northeastern Pennsylvania with the Paracyclas lirata fauna of the Portage of eastern New York; which later he demonstrated belonged in the Ithaca formation.: It is interesting, however, to re- member that farther to the southwest in western Maryland the higher Devonian faunas contain numerous specimens of Spirifer dis- junctus associated with some of the other species which professor Williams lists as diagnostic of the Chemung. (Cas ig JES MONTHLY AUTHOR’S CATALOGUE OF AMERICAN GEOLOGICAL LITERATURE ARRANGED ALPHABETICALLY. LINES, E. F. (See FULLER, M. L.) LIPPINCOTT, J. B. Water problems of Santa Barbara, California. U.S. G.S8S., Wat. Sup. & Irr. Pap. No. 116, pp. 99, pls. 6, 1905. LUTHER, D. D. (See CLARKE, JOHN M.) MARTIN, G. C. The Petroleum fields of the Pacific Coast of Alaska. Bull. 250, Wis: G. 5.,.Dp., 0+, pls. 7, 1905. MARTIN, G. C. Water resources of the Accident and Grantville quadrangles. (Wat. Sup. & Irr. Pap., No. 110, pp. 168-170, 1905.) MARTIN, G. C. Water resources of the Frostburg and Flintstone quadrangles, Maryland and West Virginia. (Wat. Sup. Irr. Pap. No. 110, pp. 171-173, 1905.) *Tbid., pp. 10-12. + Ibid., pp. 11, 76, 78. 415th An. Rept. State Geologist [N. Y.], 1898, pp. 142-148 and 17th ibid., 1900, pp. 74-81. 54 The American Geologist. June, 1905 MARTIN, G. C. Notes on the petroleum fields of Alaska. (U. S. G. S., Bull. 259, pp. 128-138, 1905.) MARTIN, G. C. Bering river coal field. (U. S. G. S., Bull. 259, pp. 140-149, 1905.) MARTIN, G. C. Gold deposits of the Shumagin islands. U. S. G. s., Bull. 259, pp. 100-101, 1995.) MARTIN, G. C. Cape Yaktag placers. (U.S. G. S., Bull. 259, pp. 88-90, 1905.) MATSON, GEO. C. Peridotite Dikes near Ithaca, N. Y. (Jour. Geol. vol. 13, Apr.- May, 1905, pp. 264-276.) McCASKEY, N. D. Fifth Annual Report of the Mining Bureau of Manila, P. Is., pp. 30, maps 2, Aug., 1904. MERRIAM, JOHN C. A primitive ichthyosaurian limb from the middle Triassic of Nevada. (Univ. Cal., Bull. Dept. Geol., vol. 4, pp. 33-38, plate. Feb., 1905.) MERRILL, GEO. P. Gold and its Associations. (Eng. Min. Jour. vol. 79, p. 992, May 25, 1905.) MILLER, W. G. Limestones of Ontario. (Rep. Bur. Mines, part ii, 1904, pp. 143, plates, 1905.) MOFFIT, F. H. Gold placers of Turnagain arm, Cook inlet. (U.S. G. S., Bull. 259, pp. 90-100, 1905.) OSBORN, HERBERT (and L. B. WALTON). Memorial of the Ohio Academy of Sciences on the death of Prof. A. A. Wright. (Science, vol. 21, May 5, 1905.) OWEN, LUELLA A. Evidence on the deposition of the Loess. (Am. Geol., vol. 35, p. 291, May, 1905.) PARK, JAMES. ; The Formation of Veins. (Eng. Min. Jour., vol. 79, p. 741, May 18, 1905.) PARK, JAMES. Contact Metamorphic Deposits. (Eng. Min. Journal, vol. 79, p. 896, May 11, 1905.) Monthly Author’s Catalogue. 55 PARK, JAMES. Theories of Vein Formation. (Eng. Min. Jour., vol. 79, p. 993, May 25, 1905.) PRINDLE, L. M. (and F. L. HESS). Rampart placer region. (U. S. G. S., Bull. 259, pp. 104-119, 1905.) PURINGTON, C. W. Methods and costs of gravel and glacer mining in Alaska. (U. S. G. S., Bull. 259, pp. 32-41, 1905.) PYNCHON, W. H. C. Drilled wells of the Triassic area of the Connecticut valley. (Wat. Sup. Irr. Pap., No. 110, pp. 65-94, 1905.) RAYMOND, P. E. Note on the names Amphion, Harpina and Platymetopus. (Am. Jour. Sci., vol. 19, pp. 377-379, May, 1905.) READ, THOMAS T. Platinum and Palladium in Certain Copper Ores. (Eng. Min. Jour., vol. 79, p. 985, May 25, 1905.) ROWLEY, R. R. Missouri paleontology. (Am. Geol., vol. 35, p. 301, May, 1905.) RUEDEMANN, R. Structure of some primitive cephalopods. (Rep. N. Y. State paleontologist, 1908, pp. 296-343, 1905.) RUSSELL, I. C. Preliminary report on the geology and water resources of central Oregon. Bull. U. S. G. S., No. 252, pp. 138, pls. 24, 1905. SHIMEK, B. Additional Note on Helicina Occulta. (Jour. Geol. vol. 13, pp. 232-238, Apr.-May, 1905.) SHIMER, H. W. Upper Siluric and Devonic fauna of Trilobite mountain. (Rep. N. Y. State paleontologist, 1903, pp. 173-270, 1905.) SPENCER, A. C. The Treadwell ore deposits. (U. S. G. S., Bull. 259, pp. 69-87, 1905.) ; SPENCER, J. W. Physiographie improbability of land at the North Pole. (Am. Jour. Sci., vol. 19, pp. 333-341, May, 1905.) SPENCER, J. W. Bibliography of submarine valleys off North America. (Am. Jour. Sci., vol. 19, pp. 341-348, May, 1905.) 56 The American Geologist. July, 1906 STEVENSON, J. J. The Jurassic coal of Spitzbergen. (Anals, N. Y. Acad. Sci., vol. 16, part 1, pp. 82-95, Feb., 1905.) STONE, R. W. Water resources of the Elder’s ridge quadrangle, Pennsyl- vania. (Wat. Sup. Irr. Pap., No. 110, pp. 164-166, 1905.) STONE, R. W. Water resources of the Waynesburg quadrangle. (Wat. Sup. Irr. Pap., No. 110, pp. 166-168, 1905.) STONE, R. W. “ Coal resources of southwestern Alaska. (U.S. G. S., Bull. 259 pp. 151-171, 1905.) STOSE, GEO. W. Water resources of the Chambersburg and Mercersburg quad- rangles, Pennsylvania. (Wat. Sup. Irr. Pap., No. 110, 156-158, 1905.) STRONG, A. M. (See ARNOLD, RALPH). TARR, R. S. Water resources o. the Watkins Glen quadrangle. (Wat. Sup. Irr. Pap., No. 110, pp. 134-140, 1905.) WAVEOR, Fano. Water resources of the Taconic quadrangle, New York, Massa- chusetts and Vermont. (Wat. Sur fTrr. Pap., No. 110, pp. 130-133, 1995.) ULRICH, E. O. (See GEO. I. ADAMS). UPHAM, WARREN. Fjords and Hanging Valleys. (Am. Geol., vol. 35, p. 312, May, 1905.3 VEATCH, A.C. (See FUELER, ma =; VOGDES, A. W. “Address on books relating to geology, minera! resources of California.’ (San Diego Acad. Nat. Sciences, vol. 1, No. 1, pp. 9-23, 1905.) ; WALTON, L. G. (See OSBORN, HERBERT). WARWICK, A. W. The Leadville District. (Min. Marg, vel. 11, pp. 430-439, May, 1905.) WELLER, STUART. A Fossil Starfish from the Cretaceous of Wyoming. (Jour. Geol. vol. 13, pp. 257-259, Apr.-May, 1905.) WEST, HE: Tin in California. (Eng. Min. Jour., vol. 79, p. 852, May 4, 1905.) Correspondence. 57 WHITNEY, F. L. The new artesian water supply at Ithaca, New York. (Wat. Sup. Irr. Pap., No. 110, pp. 55-64, 1905.) WILLCOX, 0. W. The so-called Alkali Spots of the Younger Drift-sheets. (Jour. Geol., vol. 35, p. 266, May, 1905.) WINCHELL, N. H. Deep wells as a source of water supply for Minneapolis. (Am. Geol., vol. 35, p. 266, May, 7905.) WOODBRIDGE, DWIGHT E. The Mesabi Iron Ore Range, xi. (Eng. Min. Jour., vol. 79, p. 892, May 11, 1905.) WOODMAN, J. E. Distribution of Bedded Leads in relation to mining policy. (Proc. & Trans. N. S. Inst. Science, vol. 11, pp. 163-178, Mar., 1905.) WOODMAN, J. E. Geology of Moose River gold district, Halifax County, Nova Scotia. (Proc. Trans. N. S. Inst. Sci., vol. 11, pp. 18-82, 1904.) WRIGHT F. E. (and C. W. WRIGHT). Economical developments in southeastern Alaska. (Bull. U. S. G. S., No. 259, pp. 47-68.) WRIGHT, C. W. (See WRIGHT, F. E.) CORRESPONDENCE. ESTIMATION OF THE SILICA IN THE BEDFORD LIMZSTONE —The specimen used in this work was obtained from a quarry near Bed- ford, Indiana, and it is known locally as the Bedford limestone. It is a light-colored rock, fine grained in texture, and is widely used and favorably regarded as a building material. The amount of residue insoluble in hydrochloric acid which proved to be mainly silica was determined by three different meth- ods as follows: Method 1. A grain -of the fine powder was placed in a small beaker covered with a watch glass. Dilute hydrochloric acid was added and the contents of the beaker gently heated to boiling. After standing a short time, the undissolved portion was filtered off and the weight determined. Method 2. A grain of the powder was placed in a porcelain evaporaing 58 The American Geologist. ye dish, and while covered with a watch glass, dilute hydrochloric acid was added. It was left on the water bath until effervescence ceased, the accumulations on the watch glass were rinsed off, and the evaporation continued until crystals began to appear. Then as the evaporation went forward, the substance was stirred with a glass rod until a fine dry powder resulted. This was moistened with concentrated hydrochloric acid and left on the water bath for a few moments. Dilute hydrochloric acid and water were added and after sanding a short time, the insoluble residue was filtered off, dried in the air bath, and its weight determined. The insoluble residue was obtained three different times by each of the two methods, varying the weight of the original amount taken. The results were as follows: Method 1. (a) With sone: eram "substances: cea 0.54 per cent. (b) “three grams el Sees a. Aes Oo erdic. ORO a (c) “ten f SEAN chats arererene terete OF DEE ae Method 2. (a) With tone seramieswostancer. acc. cla 0.65 per cent. (b) “three grams Sue atonal ears ke nals OSD. = sf (c) “ten * feet iS ouaisra wanes ORS5 ess = To determine further the nature of the residue, whether it was all silica, or wholly or partly a silicate, it was treated in the platinum crucible with a few drops dilute sulphuric acid, and the crucible was nearly filled with a dilute solution of hydrofluoric acid. It was evaporated on the water bath and the excess of sulphuric acid. removed with the free flame. Residue in Crucible obtained by method 1: (a)) (One V2ramesubstancerrs ceric ckereateeseae 0.13 per cent. (b) Three “ Se Se poe EAE OE ae (lee & (ce) Ten on AP ALSOP AMR aire note T ae Onda sf Residue in Crucible obtained -by method 2: (aye Oneseram substance acc mess ora sieienaeo) rele 0.13 per cent. (b) Three “ EE ATA ta wisaine Atte satis WASHOE Nee Mace (Deals we (c) Ten - SE nh Ee Setainitn crops seetacaatee hee OR aa o A blank test was made using sulphuric and hydrofluoric acid in the crucible and evaporating to dryness. No residue was ob- tained. The residue in the crucible was determined and found to be Muminum) and iron sulphatesan-:. ccs sek see aoe 0.08 % Calcium sulphate: sa anoet coerce 0.058 % Masnesiumissulphate: lyse ciecrcmke sinners wees Siaebavewnaede 0.00 0.138% Method 3. To compare the insoluble residue obtained by fusion with alkaline carbonate with the amount obtained by the foregoing methods. A gram of the fine rock powder was thoroughly mixed in the Correspondence. 59 platinum crucible with seven grams of anhydrous sodium carbonate. The sodium carbonate used was a good quality of Merck’s manu- facture. It was further purified by dissolving a quantity in water and filtering. This after fractional crystallization seemed to be entirely free from silica. The covered crucible was heated for fifteen minutes with a Bunsen flame, then with a blast lamp to complete fusion. The cooled mass was transferred to a porcelain. evaporating dish and dissolved in dilute hydrochloric acid. Evap- oration was continued on the water bath until crystals began to appear. It was then stirred with a glass rod until a fine dry powder was obtained. It was treated with hydrochloric acid as in method 2 before described. The insoluble residue obtained by this. method amounted to 0.53%. This treated with sulphuric and hydro- fluoric acids left a residue of 0.16%. The results are fairly con- cordant with those obtained by methods 1 and 2, but on account of the difficulty of getting pure sodium carbonate, and the length of time and the labor necessary to obtain fhe result, this process is not to be commended with rocks of this character. Indeed method 1 is greatly to be preferred, whenever circumstances per- mit, on account of its simplicity, and the shortness of time required. During the course of this work our attention was called to the estimation of silica as outlined by Treadwell* in his excellent treatise on quantitative analysis. After removing the insoluble residue according to method 2, it is stated that “as much as 5 per cent of the total amount (of silica) may remain in the filtrate. In order to remove this the filtrate from the first precipitate is once more evaporated to dryness on the water bath and kept on the hot water bath for one or two hours or more.” It is then filtered after treatment with hydrochloric acid and water in the usual manner. Several determinations were made in which the suggestions of Treadwell were strictly carried out. One gram, five grams and ten grams of substance were used. In no case was even a trace of residue obtained by the second treatment. The experiment was varied by using a specimen of argillaceous limestone that contained 18 per cent of silica. A second portion of residue could not be obtained from this specimen. : A complete analysis of the Bedford limestone resulted as fol- lows: (Oe (SOAS ARTA oie Es hs EES he ee ee 93.55% IIS “(CONS Soe ee ce wea ear A ae Ean Oe EE Sp et ee Rey ea 5.42% SIO oe RAC hhis Gaaks Da wea mae 0.55% LENEEE COE! Pec (7) Gat OEE Bf ie A er 0.50% 100.02% The condition of the iron was tested by placing three grams of the powdered rock in a flask of 12 ¢ ¢ capacity, fitted with a bulb * Treadwell-Hall’s Quantitative analysis, page 384. 60 The American Geologist. July, 1905 tube and Bunsen valve. The material was dissolved in a small ‘quantity of dilute hydrochloric acid. A few drops of the solutign quickly withdrawn and placed on a porcelain tile in contact with a solution of potassium ferricyanide showed a slight tinge of blue. A few drops of a solution of potassium sulpho cyanate were then quickly introduced into the flask when a red color was produced. The portion of the iron soluble in hydrochloric acid is therefore of both the ferrous and ferric forms. No attempt was made to de- termine each quantitatively on account of the small amount. The writer acknowledges his indebtedness to Alys Boies Carson for making the experiments of this investigation. NICHOLAS KNIGHT. ‘Chemical Laboratory, Cornell College, July 4, 1905, PERSONAL AND SCIENTIFIC NEWS. Pror. W. W. Mirus has been appointed state geologist of Michigan to succeed Prof. A. C. Lane. Dr. O. C. Farrineton has recently returned, froma long trip, to the Field Columbian Museum. Mr. WH. Haryey of Eveleth, Minnesota has been ap- pointed inspector of mines, with headquarters at Eveleth. Dr Joun M. Crarke. Director of Science and State Geol- ogist of New York, as well as one of the editors of this journal, has been seriously ill with appendicitis. Mr. Grorcr F. Lams, a graduate of Ohio university and later a graduate student in geology at Ohio State uni- versity, has been elected professor of Biology and Geology in Mount Union college at Alliance, Ohio. Ture “Mintinc Worip” of Chicago has recently been purchased by a new stock company. The editorial staff ‘has been strengthened and enlarged, under the direction of Meo. t.. «Daye Pror. J. Votnry Lewis of Rutger’s college will devote the summer to a special investigation of the petrography of the Newark (Triassic) traps of New Jersey and their associated copper ores for the state geological survey. Dr. M. W. Twircneir, a graduate of Columbian univer- sity, Washington, D. C., and of Johns Hopkins university, Baltimore, Md., has been elected to fill the chair of geology in South Carolina college at Columbia, S. C. Mr. Ernest C. Brown, publisher of “Progressive Age,” is preparing to publish a complete list of the engineers of Personal and Scientific News. OF America. He has listed already over two thousand and desires information concerning five or six thousand others. WaRREN UPHAM contributes a paper of eighteen pages, entitled “Geological History of the Great Lakes and Niag- ara Falls,” to the July number of The International Quar- terly. ee T. Day of the U. S. Geological Survey has re- cently made a visit to the Yellowstone Park. He is now in charge of the concentration of black sands carried on by the survey at the Portland exposition, where he also- holds the position of honorary chief of the mines department. . Mr G. K. Gizerr has given to the Department of Geol. ogy of Denison university upwards of 1,000 volumes of lit- erature, consisting of U. S. G. S. reports, state reports, re- prints, proceedings, and other valuable books. This gift is especially appreciated after having lost their library in the burning of their Science Hall. Tue Posirton oF THE LATE ALBERT A. Wrieut of Oberlin college has been filled by the election of Maynard M. Met- calf, professor of Biology in the Woman’s college of Balti- more, as professor of Zodlogy and Mr. E. B. Branson of Kansas university as instructor in Geology. Dr. Metcalf was granted a two years’ leave of absence and the work for the ensuing year will be conducted by Dr. Lynds jones, associate professor of Zoology and Mr. Branson. Tue Ser or Cuarrs illustrating the origin of certain metallic ores, prepared by C. R. Van Hise, C. K. Leith and W.N. Smith and exhibited at the St. Louis Exposition, has been reproduced in Vandyke prints for limited distribution, in response to requests for copies. The prints are four in number, iron, copper, gold and silver, and lead and zinc, each about 24 by 50 inches. A charge of 75c each is made to cover cost. Orders may be sent to C. K. Leith, Madison, Wis. Pror C. H. Hircucock, of Dartmouth college, will spend the months of July and August in the Hawaiian Isl- ands, to visit again their principal volcanoes, all of which he has ascended during his numerous former explorations of these islands. His observations this summer are for re- vision and completion of a treatise on volcanoes, and espec- ially on their very exceptional characters in the Hawaiian group. Dr. Grorce D. Husparp, instructor in geology and physical geography in Cornell university has been elected assistant professor of Geology in Ohio State university. The other members of the Geological department are Charles S. Prosser, professor of Geology and John A. Bow- nocker, professor of Inorganic Geology. In recent years 62 The American Geologist. July; 208 the department has grown very rapidly and during the last four years the number of students has nearly trebled. Dur- ing the present summer session the instruction in geology is given by Dr. Aug. F. Foerste of Dayton. ‘(Ip WAS STATED IN THE ISSUE OF SCIENCE for April 21, that the New Mexico legislature had appropriated $6,000 for a state geological survey, to be spent under the direction of the New Mexico school of mines at Socorro. We are in- formed that the only reference to such a survey occurs in the general appropriation bill and is as follows: ‘For pub- lication U. S. Geological Survey reports, to be expended under the direction of the Socorro School of Mines, or so much thereof as may be necessary, $2,500.’ ” —Sczence, A similar misstatement was published in the GroLoaIsT for April (p. 262): Tar DeLavepD Annuat Report of the Geological Survey of Michigan for 1903 is out. It consists of 342 pages and contains report of the state geologist and included papers. Among the noteworthy articles are those on the soils and vegetation of Roscommon and Crawford counties by B. E. Livingston, and notes on the waters both of the Upper and Lower Penimsulas: There are articles onthe theory ot copper deposition and the Keewenawan lodes. The report is sent gratis on payment of forwarding charges (13 cents) to teachers for professional use, editors for review and to libraries according to the rules of the Board whose office is at Lansing, Michigan. Tue Late Leaisvarure oF Inuimors established astate geo- logical survey, putting it under the immediate direction of the trustees of the state university, located at Champaign, but with an advisory board consisting of the governor, the president of the university and one other to ‘be appointed by the governor. The annual appropriation is twenty-five thousand dellars. In addition to the above the university is to have a school of ceramics, supported by an appropriation of five thousand dollars per year. This, however, will have no connection with the survey except such as common inter- est dictates. —Rolle. Congress oF APPLIED GEOLOGY. An international con- gress of applied geology was called to meet at Liege from 25 June to rt July, 1905. It took place in connection with the Universal Exposition of Liege, and of the International Congress of mines, metallurgy, mechanics and applied geol- ogy, of the last of which it seems to be an offspring. The president and the secretary of the Committee of organiza- tion are respectively Max Lohest and René D’ Andri- mont, both of Liege. Amongst the organizing members Personal and Scientific News. 63 are named the following: Ch. Barrois, P. F. Chalon, De Launay, H. Domage, E. Dubois, J. Gosselet, H. Hofer, K. Mennack. F. Laur, H. Louis, M. Lugeon, H. Potonié, Schulz-Briesen, F. Villain and numerous Belgian geologists. THE Screntiric Wortp will be specially interested to learn that Dr. G. F. Wright, is about to make an expedition _to southern Russia and the north end of the Red sea, to com- plete the investigations begun by him in 1900 and 1901, the object of which was to determine the physiographic changes which have taken place in comparatively recent times in the regions earliest occupied by man, and to ascertain the influence these have had upon the history of the human face: This expedition is made possible by a special fund pre- sented him as president of the Records of the Past Explora- tion Society for this particular work. Full reports of his investigations will appear in Records of the Past during the autumn and winter. During his trip he will receive mail, in care of the American Consulate, at the following points:—Aug. 12, York, England; Aug. 25, Copenhagen, Denmark; Sept. 8, Moscow, Russia; Sept. 15, Vladikavkaz, Russia; Sept. 25, Sevastopol, Russia; Oct. 5, Constantinople, Turkey in Bucope: Oct 15, Beirut, Syria; Oct. 25, Jerusalem, Pales- tine; Noy. 5, Cairo, Egypt; Nov. 13, Athens, Greece; Nov. Zenaples. Italy; Dec; 1, Rome, Italy; Dec. . 20, .Paris, France; Jan. 1, London, England. Butietin No. 60, oF roe Bureat or Forestry being a “Report on an Examination of a Forest Tract in Western North Carolina,” by Franklin W. Reed, will soon be ready for distribution. This report contains a comprehensive and detailed description of the forest on about 16,000 acres in the moun- tains of western North Carolina, which is to be lumbered so that its value as a summer resort shall not be impaired. This tract is typical of many others in the southern moun- tains, where undeveloped resources afford an opportunity for the practice of forestry or conservative lumbering. The conditions described in this bulletin furnish a concrete ex- ample of what such land will yield when placed in the care of a forester, who will look after its landscape features while cutting the merchantable timber. Tables of growth and yield are provided, logging and pleasure roads located, and a system of fire protection outlined. The bulletin is illustrated with a topographic map and six plates. Application for this bulletin should be made to The Forester, U. S. Department of Agriculture, Washing- tomy D.C. 64 The American Geologist. July, 1905 Tur TECHNOLEXICON oF THE SocreTy oF GERMAN En- GINEERS (short report on the state of work June, 1905). In the compilation of this universal technical dictionary for translation purposes (in the languages English, German, and French), that was commenced in 1901, about 2000 firms and individual collaborators at home and abroad are assist- ing at present. Up to now 2,700,000 word-cards have been collected. To these will be added the hundred thousands of cards that will result from the working-out of the original contribu- tions not yet taken in hand. The contributions have been called in since Easter, 1904, and most of them have already come in (up to June, 1905: 1480). The editor-in-chief will be pleased to give any further information wanted. Address: Technolexicon, Dr. Hubert Jansen, Berlin (NW. 7), Dorotheenstrasse 49. A SpeciAL SUMMER MEETING OF THE AMERICAN ANTHRO- POLOGICAL ASSOCIATION will be held in San Francisco, Cali- fornia, on August 29, 30 and 31. After the meeting there will be an excursion to Portland, Oregon, to visit the Lewis & Clark Exposition. Here an informal meeting will be held at which addresses will be made. The meeting in San Francisco will be held under the auspices of a local committee. This committee will arrange for excursions and entertainments. The headquarters of the Association will be the Department of Anthropology of the university of California at the Affiliated Colleges, San Francisco. Since special rates are being given by the transconti- nental railroads to Portland via San Francisco, it is an ex- ceptional opportunity for ethnologists and archeologists to visit the Pacific coast. Members intending to be present will please notify the secretary of the local committee, Dr. A. L. Kroeber, Affili- ated Colleges, San Francisco. Dr. Kroeber will arrange for hotel accommodation and will furnish information relative to the meeting. The amendments to the constitution proposed at the Philadelphia meeting (see Amer. Anthropologist, 1905, p 176) and at the council meeting of April 15, 1905, bavi been approved by the council, will be presented at San Fran- cisco for adoption. Mr. George Grant MacCurdy, 237 Church street, New Haven, Conn., secretary of the Association, will give infor- mation as to special railroad rates. Titles of papers should be sent to him at an early date. BIN HER (Al - THE AMERICAN GEOLOGIST, Vou. XXXVI, PLATE IIT The portrait of Prof. Wright, Vol. XXXVI, Plate If, was badly printed. please substitute this The binder will il a LIBRARY - : | te Se aoe ey, UNIVERSITY of ILLINOIS THE AMERICAN GEOLOGIST. VOL. XXXVI, AUGUST, 1905. No 2. oe ALBERT ALLEN WRIGHT. By Pror. G. F. WriGgHT, Oberlin, Ohio. PORTRAIT—PLATEH III. On the afternoon of Saturday, April 1, 1905, professor Albert Allen Wright was about his usual duties, but upon going to his study upon his wheel was suddenly seized with spasms of pain which, after continuing for twenty-four hours, ended in his death, upon Sunday afternoon. For some years professor Wright had suffered more or less from ill health, for which physicians found it difficult to account. A year of rest upon the Pacific coast in 1900 failed to bring the expected relief, but partial relief was found in a severe course of dieting. The mystery, however, was solved by a post-mortem examination, which showed that, as a result of an illness many years before, there was an adhesion between the stomach, liver, and gall bladder, which suddenly gave way, producing acute peritonitis. Thus closed the earthly career of a most accomplished geologist and naturalist, a broad-minded student of science in general, a successful teacher, an efficient man of practical affairs, and a devout Christian of such delightful personality that he won the regard of every one who came in contact with him, As so many persons have supposed that professor Wright and I were brothers, it is well to say, at the outset, that we were not, and that our relationship, if any, was so distant that it has not been traced. But twenty-five years of close association with him in college work and much longer general acquaintance had drawn me to him as to a brother, while his judgment in scientific affairs was so sound and unerring that I felt impelled to seek it at every stage of my own work. 66 The American Geologist. Avenst a0 Professor Wright was born in Oberlin, Ohio, April 27, 1846, being a son of William Wheeler and Susan Allen Wright, connected, on his father’s side, with the family of Orville Wright, and on his mother’s with the late professor Frederick Allen of Harvard university. He graduated from Oberlin college in 1865, having served for three months in Company K of the 150th Regiment of the Ohio National Guard, which was called for the defense of Washington in 1864. For two years he taught in the Cleveland institute, when he returned to Oberlin, and, like so many other dis- tinguished geologists, among whom are to be numbered pro- fessors J. P. Lesley and Edward Orton, pursued a course of theological studies, two years of which were taken in Union theological seminary, New York City, and the final year in Oberlin seminary, from which he graduated in 1870. For the following two years he filled the chair of mathe- matics and natural science in Berea college, Kentucky, after which he entered the School of Mines of Columbia college, from which he graduated in 1875. In later years his educa- tion was continued in a more general way by numerous extended expeditions into Canada, the Rocky mountains, Florida, and other portions of the Atlantic coast, while the year 1884-85 he spent in traveling in Europe. On September 21, 1874, he was married to Mary Lyon Bedortha, of Saratoga Springs, N. Y., from which union there is left a daughter, Helen M.; and August 18, 1891, to Mary P. B. Hill, of Flemington, N. J., who with a son sur- vives him. In 1874 he was called to the chair of geology and natu- ral histery in Oberlin college, a position which he filled with complete satisfaction to all for thirty years, to the time of his sudden death. He signalized his connection with Ober- lin college by establishing and fostering the laboratory sys- tem of study by students in all scientific departments, so that his pupils have shown remarkable facility in their post- graduate studies and in finding entrance to the higher spheres of scientific investigation. | But he accomplished a large amount of work outside of his classroom, as will be seen by the appended list of publi- cations. In 1874 he was engaged upon the second geolo- Albert Allen Wright— Wright. 67 gical survey of Ohio to make a report upon the lake ridges: of Lorain county. The published results of his work remain the standard source of information concerning that locality. In 1884 he was employed to make the report upon the coal- seams of Holmes county, and in 1893 he was asked to make, for the current volume of the Survey, a report on “The Ven- tral Armor of Dinichthys,” based upon the unique specimens from Lorain county preserved in the Oberlin college museum, in which he demonstrated that what are described by Dr. Newberry as jugulars are really the “companions of his anterior ventrals.” Among the most commendable aspects of professor Wright’s scientific work are those which come to light in connection with his practical interest in the affairs of the town and state. Such confidence did his fellow-citizens have in both his attainments and his character that as soon as they contemplated the inauguration of a sewer system and waterworks he was chosen by universal consent to be the leader in formulating plans. After an untold amount of ex- amination of the local conditions, and of study of the subject from every point of view, he presented plans which were ac- cepted, and which, executed under his direction, have secured to Oberlin the model equipment of the state, to which the State Board. of Health is constantly referring committees from other localities. All this was accomplished at a mini- mum of expense to the town. It is also through professor Wright’s influence chiefly that the legislature of the State was persuaded to co-operate with the United States geolo- gical survey inaugurating a topographical survey of Ohio. His papers, presented to the committees of three different legislatures, and others published broadcast throughout the state, are models both in the statement of the scientific re- sults to be published and of the practical ends to be secured, in order to justify the large appropriations made. BIBLIOGRAPHY. Lake ridges of Lorain County, Ohio. Geol. Sury. Ohio, Report, vol. II, pp. 207-210. Columbus, 1874. The coal seams of the lower coal measures of Ohio (continued). The coal mines of Holmes county. Geol. Surv. Ohio, Report, vol. V, Economic Geology, pp. 816-842. Columbus, 1884. 68 The American Geologist. GEE ee Preliminary list of the flowering and fern plants of Lorain County, Ohio. Oberlin, Goodrich, 1889. 30 p. O. Extra-morainic drift in New Jersey. Am. Geologist, vol. X, pp. 207- 216. 1892. Additions to the preliminary list of the flowering and fern plants of | Lerain County, Ohio. Oberlin, 1898. 11 p.0O. (Oberlin College Dept. Laboratory bulletins, No. 1, supplement.) Nikitin on the quaternary deposits of Russia and their relations to prehistoric man. Am. Journal of Science, vol. XLV, pp. 459- 468. 1893. Older drift in the Delaware Valley. Am. Geologist, vol. XI, pp. 184- 186. 1893. On the ventral armor of Dinichthys. Ohio Geol. Surv., vol. VII, pp. 620-626. 1893. Ventral armor of Dinichthys. n. p. n. d. Am. Geologist, vol. XIV, pp. 313-320, pl. IX, figs. 1-2. 1894. Limits of the glaciated area in New Jersey. Geological Society of Am., Bulletin, vol. V, pp. 7-13. 1894. Address upon a topographic survey of Ohio. n. p. 1896. 11 p. D. Ohio boulders containing huronite. Ohio State Academy of Science, 5th An. Rep. 1897. Summaries in Systematic Zoology. Oberlin 1897. 35 p. O. Trans. from Hertwig, Richard. Lehrbuch der Zoologie. (Ober- lin—College Dept. Laboratory bulletins, No. 5.) With W. G. Tight, and others. A topographic survey of Ohio. n. Dp. 219035 a4 eps: Laboratory directions for the study of Amphioxus. Oberlin, Good- rich, 1902. 25 p. O. (Oberlin—College Dept. Laboratory bulle- tins, No. 11). Our smallest Carnivore. Ohio Naturalist, vol. V, pp. 251-254. 1905. A topographic Survey of Ohio. n.d.7 p. Charles Vinal Spear. n. p. n.d. 55 p. Por. Il. O. Classification of the animal kingdom. n. p. n. d. 35 p. O. Trans. from Hertwig, Richard. Lehrbuch der Zoologie. : Concerning a topographical survey. n. p. n. d. 4 p. Early embryological stages of amphioxus. n. p. n. d. 4 p. General Zoology. n. p. n.d. 4 p. Herbarium-making. n. p. n.d. 7 p. O. Optical properties of rock-making minerals n. p. n. d. 8 p. Rocks. on. ds ip: Students’ collection of fossils. n. p. n. d. 4 p. The dissection of molgula. n. d. 7 p. Relations of the Igneous Rocks—Crosby. 69 GENETIC AND STRUCTURAL RELATIONS OF THE IGNEOUS ROCKS OF THE LOWER NEPONSET VALLEY, MASSACHUSETTS. [Il.] By- W. O. Crossy, Boston, Mass. PRE-CARBONIFEROUS INTRUSIVES. The earlier or pre-Carboniferous intrusive rocks of the batholite include the following types: granite porphyry, quartz porpryry, felsite and acid andesite. The first three are acid and agree closely in composition, as stated above, with the sedentary types of the batholite, so that they may fairly be regarded as later extravasations from the deeper parts of the same great body of magma. The fourth type, on the other hand, is of distinctly sub-acid or neutral com- position, as a partial analysis accompanying Dr. Bascom’s description clearly shows. Furthermore, the dikes of this relatively basic type are, according to the rather meagre but quite satisfactory evidence, older than all of the acid intrusives, suggesting eruption from a source below the normal granite and hence during a time (possibly of mark- ed elevation and erosion) when the batholite proper was congealed throughout its entire thickness. The acid intrusions, on the contrary, including both dikes and necks, may, in the main at least, as previously indicated, be correlated with the subsidence ushering in the sedimentation of Carboniferous times and accompanied by a rise of the isogeotherms sufficiently marked to reliquefy a portion of the ancient acid magma. This correlation is confirmed by the close agreement in composition of the acid intrusions and the normal granite,—for the unquestion- able connection of the acid intrusives (both dikes and necks) with the acid effusives or lavas, which rest uncon- formably upon the deeply denuded surface of the batholite, shows that in origin the intrusions are separated from the sedentary zones of the batholite by a vast time interval during which the magma must have been mainly solid to have escaped marked chemical differentiation. Acid Andesite Dikes—This is a rock of distinctly neu- tral composition, anlyses showing from 60 to 62.8 per cent. of silica; and Dr. Bascom’s observations indicate a horn- blende-bearing biotite andesite. A single dike only has 70 The American Geologist SurCs oes been studied in detail; but it is known to represent a more or less extensive Series, the acid andesite not having been distinguished heretofore from basic andesite and green- stone diabase. This dike.begins in the fine granite on Heron street near Washington street and, with a normal breadth of 20 to 25 feet, has been traced northwesterly, parallel with Cottage avenue, into the normal granite and for o total distance of nearly half a mile. . It is clearly cut by typical dikes of quartz porphyry and felsite; and the acid andesite occurs as angular inclusions in a great dike of granite porphyry. These relations give it at once a unique position among the basic intrusives of this area and, so far as known, of the Boston basin, by definitely fixing it, chron- ologically, between the batholite and all of the acid intru- sives. Comparison is suggested at once with the more basic, pre-granitic dikes (diabase) in the Cambrian slates of the Blue Hills.* The latter are the only basic dikes in the Boston basin known to be older than the granitic series of the Complex; and the West Roxbury dike just de- scribed is the first relatively basic dike in the Boston basin known to be intermediate in age between the sedentary . zones and the acid intrusions of the complex. Granite Porphyry and Quarts. Porphyry Dikes,—In this instance, also, the detailed study has been limited to what is, virtually, one large and complex example ;-but ‘the general conclusions thus reached are definitely known, te be applicable to ‘an extensive series of dikes.. -The.fine granite of Bearberry hill in the northeast part of the Stony Brook reservation is traversed in a general northwest-south- east direction by a vertical dike of quartz porphyry 100 feet wide. The greenish gray, aphanitic groundmass of the porphyry is crowded with conspicuous phenocrysts of feld- spar up to one-half, and even three-fourths, of an inch in length, while the more scattering, rounded blebs of quartz are commonly one-fourth to one-half inch in diameter. Al- together it is a striking rock and one readily recognized and traced. The quartz porphyry is densely felsitic near the contacts, which are firmly welded, irregular in detail, and further characterized by occasional inclusioris of the fine * @Occas, Paners, BY So. IN. Hed is sk: Relations of the Igneous Rocks---Crosby. 71 granite in the quartz porphyry and minor apophyses of the latter in the former. On this hill, also, the quartz porphyry dike is cut by a four-foot dike of compact and purple felsite, and gives off an oblique branch 20 feet wide, traceable for a thousand feet, and cut by another felsite dike 10 to 15 feet wide. The phenocrysts of the branch dike are relatively small and inconspicuous, and comparable in size with those of the contact zone; while this contrast between the main dike and its branch proves that in neither case can the phenocrysts be regarded as antedating the intrusion of the magma. On the other hand, the lithologic resemblance of the branch dike to the quartz porphyry phase of the con- tact zone must be regarded as a mere coincidence, since we have to do in the one case with the earlier phase of the bath- olite, and in the other with relatively late intrusions cutting, as we shall see, all of the sedentary zones of the batholite from the normal granite to the quartz porphyry. Southeastward, the main dike is traceable across the reservation boundary and nearly to the Boston-Hyde park line, where it is seen to cut the quartz porphyry of the contact zone and the enclosed masses of Cambrian slate. In the opposite direction from Bearberry hill, across the drift-floored valley of Turtle pond and beyond Washington street, in the large Cottage avenue quarry in normal gran- ite, capped by fine granite, and exactly where the great dike of quartz porphyry might be expected to reappear, we find instead, and with the same trend, a dike of profusely por-. phyritic granite porphyry, 30 to 50 feet wide. With aphanitic and firmly welded margins, it cuts, clearly and unmistakably, both the normal and the fine granite; and’ it is, in turn, cut squarely across by a small dike (2 to 4 feet) of felsite in which the fluxion structure parallel with the irregular walls is beautifully developed. Apparently, there is no reason to doubt that this intrusive granite por- phyry which Dr. Bascom regards as essentially identical in composition with the normal granite, is also simply a more crystalline phase of the intrusive quartz porphyry, the two rocks being part of one and the same continuous dike; and facts yet to be noted abundantly confirm this conclusion? 72 The American Geologist. Atgret ae The next outcrop of this dike, where it crosses Hieron street, is also granite porphyry; but beyond this the quartz porphyry phase recurs, and the dike, now 75 feet wide, is lithologically indistinguishable from the Bearberry hill sec- tion. From this point on, it is near to and approximately parallel with the dike of acid andesite previously described; and the latter is cut by minor dikes or apophyses of quartz porphyry. The outcrops of both dikes are now interrupted by a swamp, beyond which the dike of acid andesite con- tinues unchanged, while the porphyry dike, now 80 feet wide, is once more a typical granite porphyry, apparently repeated by an oblique strike fault and, as_ previously noted, enclosing angular fragments of the acid andesite. Thus twice in a total distance of a little more than a mile, the quartz porphyry gives way to granite porphyry. In neither case, unfortunately, can the transition be fully traced; and yet we may not reasonably doubt its reality. This remarkable and rhythmic textural variation in the con- tents of one and the same continuous fissure may, per- haps, be regarded tentatively as finding its most natural explanation in varying original depths of solidification. That is, if we may assume a natural gradation upward in the dike from granite porphyry to quartz porphyry, then a moderate ainount of subsequent displacement, or even of unequal erosion, might suffice to give the alternations of texture which the outcrops now show. - In this connection it may be noted that in the lowest outcrop of the main dike, at the western base of Bearberry hill, the quartz porphyry is well advanced in the change to granite porphyry. Itisa fair corollary of this explanation that the granite porphyry should be found chiefly in the normal granite, and the quartz porphyry in the fine granite. This relation is clearly realized in part; and would, perhaps, be more fully realized, but for the fact that, as we suppose, the batholite suffered strong and unequal erosion before its injection by these acid intrusives. Felsite Necks.—Besides its abundant occurrence in effusive forms or surface flows, the devitrified rhyolite (aporhyolite) or felsite has an important development in necks and dikes, which are undoubtedly contemporaneous Relations of the Igneous Rocks---Crosby. 73 with the acid effusives; and nowhere, apparently in the Boston basin, are normal effusives more clearly or typically developed. Some of the felsite dikes are large enough to be regarded as the vents of effusive masses; and very prob- ably several of them are deeply denuded necks. The more typical and unequivocal necks, however, are less dike-like in outline and far more diversified in structure, consisting chiefly of clastic lavas—agglomerate and tuff—suggestive of explosive eruptions toward the end of the volcanic activ- ity and following more quiet liquid effusions. Three essen- tially distinct vents have been more or less fully worked out; and it is considered not improbable that others await recognition in the felsite areas. This appears the more likely in view of the fact that acid lavas of fluidal and auto- clastic types, that is, lavas which were stiff enough at the time of their effusion to develop fluxion lines, or even to be- come brecciated by their own flow, would not spread far from the vents through which they reached the surface. We must recognize also the extreme probability that some vents are still concealed by their own sluggish effusions or by later sediments. The three vents referred to as more or less fully identified are near the heart of the complex and bordered either wholly or in part by the sedentary zones of the batholite, including the normal granite, fine granite and quartz porphyry; and evidence is not wanting that they are, in each case, located on important displacements, one indication of this relation being elongation in a definite direction, the outlines being distinctly lenticular. The West Roxbury Neck,—This neck is the most clearly exposed in outline and in structural detail, and probably the largest, as it is certainly the most indubitable of the series. It occupies approximately the irregular triangular area bounded by Grove, Center, Stimson and Washington streets in West Roxbury, near the Dedham line. It is elongated in a general northwest-southeast direc- tion, the extreme dimensions being approximtaely 1200 by 3500 feet. The major axis coincides in position and trend with the common boundary of the fine granite and the western area of normal granite, the evidence being quite conclusive that this line marks an important displacement. August, 1 056 74 The American Geologist. The sharp definition of this neck, with its continuous rim of granite, is, of course, chiefly due to the fact that erosion has removed the last vestige of the effusive felsite which we must assume to have once covered its site and a wide area of the enclosing granites. Not to classify this sharply defined body of acid lavas as a true neck or vent would seem to necessitate regarding it as a depressed fault block or graben, a remnant of a once widely extended volcanic sheet covering the granites which has escaped erosion through the accident of displacement. But the varied and _ prevailingly clastic character of the lavas and the general structure of the mass are, at least, highly suggestive of a vent, and force the conclusion that there must be a vent somewhere in this part of the com- plex. Although, omitting intersecting dikes of felsite, an- desite and diabase, the neck is almost wholly composed of effusive types of felsite; it is yet, quite independently of the dikes, highly diversified in composition and structure— a constantly varying complex or chaos of fragmental, fluidal and compact or structureless lavas. The clastic phase, ranging from the finest tuff to the coarsest breccia or agglomerate, largely predominates and gives character to the whole, leaving little room to doubt that the later eruptions, at least, from this vent were in part explosive. Although varying greatly in azimuth and inclination, and usually much contorted, the normal attitude of the flow structure of the felsite is parallel with the axial plane of the neck, or, in the peripheral portions, with the proximate wall of granite. The interest of the peripheral phenomena culminates in the southeastern extremity of the neck, where it is continued in the shattered zone of granite in which it had its origin as a complex of granite and _ felsite, the granite being cut in all directions by irregular branching and coalescing dikes of the felsite, which is brecciated, banded, compact or porphyritic by turns and encloses many large and small angular fragments of the granite. While we need not doubt that, the fragmental lavas are, in the main, true pyroclastics, the product of explosive eruptions, it is very probable that they are in part auto- clastics, or breccias resulting from the continued movement Relations of the Igneous Rocks---Crosby. 75 of the magma after it began to stiffen and solidify. The distinction of these two types in the field must usually be a puzzling matter, so much depending on the nature of the matrix or ground mass; but it is assumed here that local homogeneity of composition (not of texture) and absence of granitic debris are characters belonging more normally to the autoclastics. In considering the distinction and probable relative abundance of the pyroclastic and auto- clastic lavas, both of which are undoubtedly prominent features of this neck, and may also be designated, respec- tively, agglomerate and breccia, we may properly take ac- count of the possibility that the eruptions were subaqueous, at least in part, and note the cracking and shattering of the lava that would follow its sudden quenching. It is doubtful, however, if much of the breccia has the crackled character, with accurately fitting fragments, which this explanation would require. Nevertheless, the presence of water is plainly suggested by the rather distinct stratifica- tion of some of the finer tuffs, such as may be observed in the ceritral part of the neck especially. Attention is thus directed to one of the most interest- ing and puzzling features of the neck. This is a very com- pact gray, slaty-looking rock, irregular masses of which are enclosed in the more normal or unquestionable agglomer- ate and also in the fluidal felsites and occur only in the western central portion of the neck, all the outcrops being included within an area about one thousand feet long in a north-south direction and perhaps half as wide. This material, which may be as distinctly, evenly and finely, or as obscurely, stratified as any slate, was at first mistaken for an:older slate enclosed in the volcanics. But further study of the field relations showed that it must be contem- poraneous and essentially a tuff or consolidated ash. As noted by Dr. Bascom, this conclusion is confirmed by both the microscopic and the chemical analyses. The combined alkalies are far higher than for a normal slate and agree closely with those of the felsites. These masses range in extent from a few inches: to many feet. They are some- times ill-defined, cloud-like patches in the lavas; but more commonly-they are. Sharply outlined and the contacts with 76 The, American Geologist. Annet the felsite are unquestionably igneous, being firmly welded and the sediment well baked for a breadth of one to several inches. Even closely adjacent masses do not usually agree in dip and strike; but the relations are what might be ex- pected in the case of a bed or beds of imperfectly consoli- dated ash disturbed by later eruptions, largely of an ex- plosive character. The close relation of the consolidated ash -or slaty tuff to the felsite agglomerate is clearly indi- cated in some instances by the intercalation of visibly clas- tic layers. Finally, we may regard the ash as the finest product of an explosive eruption which was in some sense subaqueous, closely followed by eruptions which were only in part of an explosive character, yielding, besides the true agglomerates, compact, fluidal and autoclastic felsites in- tersecting and enclosing, alike, the agglomerate and the ash. ‘Accepting the West Roxbury neck as a true volcanic vent, aS apparently we must, it may be assumed to have originated in a more or less complex and branching fault fissure; and the local widening of such a fissured zone to the present breadth of the neck when it finally became the locus of vulecanism would be a natural consequence of the explosive action of which we have such ample evidence. In other words, we need not assume that the granite was melted away, or forced out en masse, Pelée fashion; but it is sufficient to assume a splintering and shattering of the granite walls under the influence of shock and heat. The tesulting granite debris would be borne upward by the constantly increasing volume of viscous lava made possible by the widening of the vent, and finally discharged, largely through the agency of violent explosions. This explana- tion, the essence of which is a gradual crumbling and ex- foliation, accompanied by cracking and _ rending of the granite walls of the primordial fault fissure, accounts for the general diffusion of granitic detritus through the clastic lavas, as well as for larger, isolated masses of granite which now add to the diversity of the neck. The Hyde Park Neck.-—This large and composite neck occupies a more central position than the West Roxbury neck in relation to the complex; and presents some other distinguishing features. It is, probably, best regarded, in Relations of the lgneous Rocks---Crosby. ——-77 detail, as two necks developed on fissures, approximately parallel with the major axis of. the West Roxbury neck; but converging irregularly northwestward, near the Cam- brian outliers; and the united axes might be regarded as continued in the great dike of quartz and granite porphyry. Where most widely separated and most distinctly developed as necks, these fissures are clearly compensating displace- ments bounding a depressed area approximately half a mile wide. . The southwestern fissure, designated the Bold Knob neck, shows a wall of the massive quartz porphyry of the contact zone bordered on the northeast by several hundred feet in breadth of coarse felsite agglomerate, the felsitic matrix of which is packed with large, angular fragments of both felsite and quartz porphyry. Northeastward, or away from the wall of quartz porphyry, the agglomerate becomes rapidly finer and shades off into fluidal, spheru- litic and other obviously effusive forms of felsite. Similar- ‘ly the northeastern fissure, known as the Grew’s Woods neck, shows an immense mass of exceptionally coarse ag- glomerate sharply limited on the northeast by normal gran- ite. The agglomerate has a maximum breadth of nearly a thousand feet, passing gradually, as before, into the effu- sive felsites, which are continuous over the area interven- ing between the two bodies of agglomerate. Not only has the effusive felsite discharged by flow and explosion from these fissures overspread the depressed area which they bound; but from this expanding area, as from a cornucopia, the felsite flows have spread eastward over a large part of Hyde Park and into Dorchester and Milton. Unlike the West Roxbury neck, and on account of the general east- ward inclination of the geological structure of the district, erosion has not cut deeply enough to remove entirely the effusions of this most eastern of the recognized felsite necks. Felstte Stocks.—Besides the large and essentially in-’ dubitable necks of acid lava described in the preceding pages, we must, as previously noted, recognize several more ot less probable stocks or plugs of felsite in the sedentary zones of the batholite. These masses, which may, perhaps, 78 The American Geologist. August, 1905 best be regarded as more deeply denuded as well as smaller necks, are intermediate, in size at least, between the un- doubted necks and the normal felsite dikes. They are related to the necks in form and to the dikes in lithologic character, lacking entirely the clastic and fluxion characters and the general structural heterogenejty of the necks. One difficulty in regarding them as dikes is that they do not appear to occupy dynamic fissures, being chimney-like tather than dike-like in form. The clearest examples are roughly circular or elliptical plugs 200 to 300 feet in diam- eter, isolated in, and enclosing numerous fragments of, the normal granite. The rock, although felsitic in general as- pect, is, perhaps, better described as a dense, non-porphy- titic microgranite. It is essentially homogeneous and structureless, except for an indistinct peripheral zone of true felsite, in part fluidal. Felsite Dzkes.—In the general view the entire area of the complex appears to be traversed by dikes of felsite. They are, however, especially characteristic of the seden- tary zones of the batholite and the felsite necks, and are observed less commonly in the effusive felsites. In spite of the fact that they sometimes cut both the felsite necks and flows, the dikes, as a whole, are undoubtedly best re- garded as essentially contemporaneous with the acid vol- canics, and we may fairly suppose that. in some instances they have formed effective vents. We have seen that they intersect the great dikes of quartz porphyry and granite porphyry; but here, again, an important difference of age is not, apparently, a necessary inference. The relation of the felsite dikes to the necks is in some cases distinctly radial; but a broader view shows that with few exceptions they tend to be normal to the major axes of the felsite necks and the fracture zones in which the necks have been developed. The prevailing trend, therefore, is northeaster- ly and southwesterly. In the extension of the axial shear zone of the West Roxbury neck, the felsite forms a plexus of irregular intru- sions, which branch and coalesce in a quite remarkable way; while the true dikes represent the filling of compara- tively simple and sharply-defined transverse fissures due, Relations of the Igneous Rocks---Crosby. 79 perhaps, to torsional stresses accompanying the shearing. _ The felsite dikes range in size up to a hundred feet or more; and they can be traced in some instances for a good fraction of a mile; but the correlation of individfial outcrops is often difficult because of marked irregularities of form and trend. As described by Dr. Bascom, the felsite of these dikes is mainly either densely compact or, more commonly, inconspicuously porphyritic. In general, and as might nat- urally be expected, the larger dikes have porphyritic centers and nonporphyritic or compact borders; while the smaller dikes are often nonporphyritic throughout. With few ex- ceptions, the peripheral portions of the dikes exhibit more or less distinct, and often very marked, fluidal structure parallel with the walls; and the smaller dikes may be char- acterized by the fluxion lamination through their entire thickness. The large dikes, also, are usually dark red or purple in the middle portion and greenish gray along the borders ; while the small dikes are commonly gray across the entire section. It appears probable that the normal orig- inal color of the felsite was gray, that it was subsequently reddened by oxidation and later bleached by deoxidation and leaching along the borders. The greenish color of the periphery is, however, according to Dr. Bascom’s observa- tions, to be connected, in most cases at least, with a more or less marked epidotization, often followed by hydration and the development of pinite; and not infrequently a bor- der of nearly pure, soft, green pinite has resulted. PRE-CARBONIFEROUS EFFUSIVES. Effusive Felsite or Normal Aporehyolite—The acid effusions of the vents described in the preceding sections, and, doubtless, of other vents still entirely concealed by the effusives, probably constitute for the Neponset valley, a more or less continuous sheet of lava chronologically and stratigraphically intermediate between the denuded surface of the batholite and the Carboniferous sediments and dis- tinctly unconformable in its relations to both. The petro- graphic and chemical characters of the effusive felsites have been fully described by Dr. Bascom. ‘The original textural variations are most notable, including compact, fluidal, spherulitic, and clastic forms. Although the surface ex- 80 The American Geologist. eneuein se posures are numerous and instructive, by far the most com- plete section of the felsites was that afforded temporarily during the construction of the Stony Brook-Neponset tun- nel, nearly a mile long, of the High-level sewer. This shows the felsites resting upon both the normal and fine granites at points remote from the nearest surface exposures of these rocks. The fiow structure of the felsites, originally hori- zontal, is now everywhere highly inclined and chiefly ver- tical, showing that the plication of the Carboniferous sedi- ments was shared by their volcanic floor. As to the orig- inal or normal thickness of the acid effusives of the Nepon- set valley, we have no reliable data; but it was quite cer- tainly to be measured by hundreds and probably not by thousands of feet. CARBONIFEROUS VOLCANICS. The volcanic rocks definitely known to be contempo- raneous with the Carboniferous conglomerate of the Nepon- set valley include a moderately acid type—trachyte, and a moderately basic type—andesite. The andesite largely pre- dominates; but the trachyte is, in the main at least, the older and may, perhaps, be regarded as in some sense a transition type between the felsite and andesite. A potraehyte.—As described by Dr. Bascom, this is a coarsely and profusely porphyritic rock of highly feldspathic composition, with albite as the predominating feldspar. Dr. Bascom shows that the chemical analysis of this rock con- firms its classification as a soda-trachyte in which diopside must have been an original constituent; or, having regard for its present altered condition, it may be more precisely defined as a soda-apotrachyte. This rock has been recog- nized as forming one small flow’ conformably interbedded with the conglomerates of the Central Avenue district in Milton, and a probable vent, in part of agglomeratic struc- ture, on the New England railroad north of River street, Hyde Park. The latter occurrence was. intersected and more fully exposed by the Stony Brook-Neponset tunnel. A poandesite-—This important volcanic is described by Dr. Bascom as an aphanitic rock of dark purplish and greenish tints in which the original constituents are mainly altered to calcite, chlorite, epidote, quartz and other second- Relations of the Igneous Rocks---Crosby. 81 ary species. The microstructure is commonly trachytic and inconspicuously fluidal and porphyritic; and the effusive phases are often amygdaloidal or clastic. The distinguish- ing feature, chemically, as for the trachyte, is found in the high percentage of soda; and the extensive mineralogic alteration, without obliteration of original structures, makes this, therefore, a normal soda apoandesite. In areal extent and structural value the Carboniferous andesite is comparable with the pre-Carboniferous felsite; and like the felsite, it is found in the three general modes of occurrence—necks, dikes and flows. The bedded lavas, both acid and basic, of the Neponset valley are believed to be exclusively contemporaneous. The andesite dikes are very numerous; and they are found in all parts of the complex—cutting the successive zones of the batholite and its cover of acid lava ({felsite), and cutting also the acid dikes of various types, including the porphyry dikes, and the necks, stocks and dikes of fel- site. In distribution, trend, form and size they are com- parable with the felsite dikes; and the profusion of the basic dikes clearly indicates a very general and extensive fissur- ing of the subcrust during the subsidence which permitted the deposition of the Carboniferous conglomerate. It is not improbable that some of the andesite dikes have formed effective vents. But of unequivocal or nor- mal necks there are no indications in the sedentary zones of the batholite or in the vicinity of the felsite necks; but they are to be found farther east, in the effusive felsites, the clearest examples occurring on either side of the Nepon- set, in the Mattapan district of Dorchester and the Colum- bine district of Milton. These vents are decidedly elon- gated or fissure-like ; but they are readily distinguished from the andesite dikes by even greater irregularity of outline and especially by the heterogeneity of structure and the prevalence of coarsely clastic or agglomeratic lava. The evidence is quite as clear as for the dikes that the andesite is younger than the effusive felsites. The andesite flows, like the dikes, are chiefly aphanitic, but embrace, also, amygdaloidal and scoriaceous forms; and in the western part of the field, especially, bedded tuff and 82 The American Geologist. August, 1905 agglomerate, the product, probably, of explosive submarine eruptions, are prominently developed. The contempora- neous relation of the effusive andesite and the conglomerate is especially clear for these fragmental varieties ; but hardly less so for the regularly interbedded flows in the Central avenue and other parts of the field. The transverse sec- tions of individual flows are, in some instances, very in- structive, showing a normal gradation upward from densely aphanitic to amygdaloidal and scoriaceous forms of lava. DIABASE DIKES. As previously intimated, the diabase dikes of this area, as of the Boston basin generally, are referable to two dis- tinct series—distinct in age, trend and lithologic character. We may properly emphasize the chronologic distinction, as of greatest geologic significance, by designating these two series, provisionally, the Carboniferous and the Triassic. Evidently, the diabase dikes are not related in origin or composition to any of the other igneous rocks of the dis- trict ; and in size, regularity and continuity the two systems are essentially similar and normal. Carboniferous Diabase Dikes — The normal trend of the numerous dikes of this series is approximately east- west; and they rarely vary more than thirty degrees from the normal. Although commonly approximately vertical, they are more likety than the Triassic dikes to exhibit a dis- tinct hade, especially in the sedimentary terranes, the mani- fest tendency being to conform with the strike joints of the enclosing formation. In other words, these are longitudin- al dikes, traversing a series of unsymmetric folds, and sym- pathizing in attitude with the tension planes of the flexures, having been developed during a period of folding and strike or thrust faulting. In the dikes of this series transverse columnar jointing is rarely distinctly developed. Litho- logically they are rather fine-grained greenstones, the orig- inal cr normal constituents having suffered extensive chlo- ritization and eptdotization, in consequence of which the diabase is somewhat immune to kaolinization and to be reckoned among the more resistant rocks of the region. Triassic Diahase Dikes—The rather infrequent dikes of this series adhere very closely to a north-south trend and Stratigraphy of Kansas Permian---Beede and Sellards. 83 vertical attitude, a hade of even a few degrees being very unusual. Their relation to the general geological structure of the region is distinctly transverse; and, evidently, they. date from a period of gravity faulting without folding, such as the Triassic is known to have been. Transverse colum- nar jointing is commonly well developed; the greenstone alteration is wanting; and the rock yields readily to kaolin- ization, the tendency to pass by spheroidal weathering to a rusty brown earth being a marked feature of this diabase. STRATIGRAPHY OF THE EASTERN OUTCROP OF THE KAN- SAS PERMIAN.* By J. W. BEEDE and E. H. SELLARDs. PLATES IV--V. According to Prosser* and Frech?t, the Wreford lime- stone may be considered the base of the Kansas Permian. The writers’ studies are at present confirmatory to this view. From a geographic standpoint this is a most fortu- nate occurrence as this limestone forms one of the most striking and persistent escarpments in Kansas. It is the most easily mapped formation in the state with the possi- ble exception of the Florence flint, sixty feet above it. The northern two-thirds of the outcrop has already been worked out and discussed in greater or less detail, and is fairly well known, but this can hardly be said of the southern third. The object of the present paper is to give a general- ized map of the outcrop, so far as determined, and to furnish an idea of the stratigraphy, throughout the length of the strike in Kansas—a distance of over 200 miles while the ex- tent of the outcrop is several times as great. NATURE OF THE OUTCROP. In the region north of the Kansas river the escarpment formed by the Wreford limestone is frequently fainter than that of the Florence flint and Fort Riley limestone. This is true of most of the Blue river region north of Garrison. The Cottonwood limestone escarpment is subordinated in *Published by permission of the director of the University Geologi- cal Survey of Kansas. + Jour. Geol., x, pp. 709, 710, 121-724, 1902. +t Lethaea Palaeozoica, II, Lief. 2, p. 378, &c, 1899. 84 The American Geologist. August eee the northern third of its outcrop where the Wreford lime- stone and Florence flint appear in the same bluffs, as in some localities in the Blue river region. However its out- crop is always strongly marked when it is found at consid- erable altitudes above drainage level or well removed from the flints, as at Manhattan, Frankfort, Alma, etc., except when deeply drift covered as near Summerfield. In the central region, from the Kansas river south to the vicinity of Reece, the Wreford limestone is best devel- oped and forms a very strong escarpment with the Flor- ence flint forming another just above and _ west of it. Throughout this region as far south as Bazaar, Chase Co., the Cottonwood limestone escarpment retains its sharp out- line and whitish appearance. For the entire distance from the Nebraska line the Cottonwood limestone retains its striking peculiarities which are so distinct that even an amateur would not overlook it. The same may be said of the Florena shale lying upon it. South of the latitude of Bazaar both these layers lose their distinctive characters and cease to be of great importance as horizon markers. Whether or not they extend across the southern part of the state as distinct strata can only be determined by care- fully tracing them the entire distance. In the southern region, except, perhaps the southern fourth of it, the Wre- ford limestone escarpment becomes somewhat accentuated, where it actually reaches the crest of the ridge. This is due as much to the drainage as to the relative importance of the stratum which is really thinner here than it is farther north. At Beaumont and Grand Summit it has been re- moved from the top of the escarpment. At the former place it occurs at the front of the ridge some distance north and south of the railroad but falls back to the middle of the town and is lower in altitude than the railroad grade at the crest of the escarpment on account of the westerly dip of the rocks. This is more strikingly the case at Grand Sum- mit where the Wreford limestone and some ninety feet of underlying rocks have been removed along the railroad as far west as Grouse creek, west of Cambridge. About two miles north of Grand Summit it appears in the top of the escarpment and also forms a high ridge west of the town, Stratigraphy of Kansas Permian---Beede and Sellards. 85 as will be noted later. South of this region local structures come to be of some importance and the stratigraphy has not been worked out in detail. Just east of Dexter it may be seen dipping sharply into the ground to the eastward while the general dip is to the west. As far south as Reece the Florence flint reaches nearly to the edge of the escarpment forming a second prominent bench. South of this it becomes, frequently, less distinct— except in the region of Burden, and comes in in the back- slope toward the Walnut river forming a second escarp- ment. It is impossible to locate the Cottonwood limestone with certainty here by its lithologic or other characters. All the limestones of any considerable importance are ex- cellently shown in the numerous cuts and exposures but none of them possess the typical appearance of the Cotton- wood. The writers are of the opinion that it is continuous with changed lithologic characters throughout this region, but this is by no means certain. It has never been traced to the southern limit of Kansas and “into Oklahoma” by any Kansas geologist.* The statements of Keyes were probably based on Haworth’s reconnaissance map published in the first and second reports of the Kansas survey,t which was probably based on Adams’ section from Galena to Wellington.t If the Cottonwood limestone extends this far south the map mentioned is not much in error as to its general location. On this map the Cottonwood limestone is marked as the upper limit of the Coal Measures and the rocks above are indicated as Permian in accordance with Prosser’s earlier opinion.§ The outcrop of the Florence flint and Fort Riley lime- stone closely parallels the outcrop of the Wreford limestone across the state and could be represented in a general way by a line close to the line on the accompanying map, but lying just west of it. The same would be true of the Cot- tonwood limestone as far south, or a little farther, than the latitude of Emporia but lying just east of the Wreford lime- stone. In such places as Manhattan, Frankfort, and Mill * Keyes, Amer. Geol. xxiii, pp. 303 and 311. + Univ. Geol. Surv. Kans., I, pl. xxi, 1896; II, pl. xlviii, 1897. + Op. Cit., I, pp. 16-20, 1896. § For the original classification and the references to the literature see, Jour. Geol.. III, pp. 682-705, 764-800 and especially chart p. 800, 1895: For revised classification see Ibid. x, pp. 703-737, 1902. 86 The American Geologist. Augeys tS0K creek, in Wabaunsee county, there would be some error in the latter statement, but in general it would be true. DETAILS OF STRATIGRAPHY. In order to give a clear idea of the stratigraphy of this horizon throughout its great extent of outcrop it will be necessary to discuss each of the several associated forma- tions and give detailed sections of well distributed ex- posures. As already stated the escarpment of the “Flint hills” (formed by the Wreford limestone, Florence flint and Fort Riley limestone) is so marked a feature that it may be traced across the state without difficulty. Quite as striking still is the great uniformity of the formations associated with the escarpment. Northern province: n 1858 Henry Englemann passed over this region and briefly discussed the rocks, probably in the vicinity of Frankfort and Marrett.* In 1881 Broadhead published a paper on the “Geology of the Central Branch railroad’’* giving sections, particularly at Frankfort. These papers are discussed by one of the writers in the Kans. Univ. Quart., IX, pp. 191-202. In 1895 Knerr ran a section over the same route? The Nebraska area has been pretty thoroughly dis- cussed by Knight.8 The writers have been over the Blue Springs (=Wymore), Nebraska area and studied his sec- tions in a general way. According to Knight’s section the thickness of the Florence flint.in the bluffs opposite Blue Springs, numbers 5 to 7 of his section, is 19 feet 2 inches, with 13 feet, numbers 8 and 9, of the Fort Riley limestone exposed above it. At the Crusher quarry, near the B. and M. R. R.—U. P. junction south of Blue Springs we measured the section of the Florence flint, finding it to be 19 feet 6 inches with a four foot layer of limestone beneath. Includ- ing this limestone, which was not included in the flint in Knight’s section, the total thickness would be 23 feet 6 inches. This lower layer is somewhat fossiliferous. Just north of the junction beneath the U. P. bridge over the little « Simpson, Expl. Exped. Gt. Basin, Utah, p. 264, 1859. + Kans. City Rev. Sci. and Ind., V, nv. 119 et sea. t Univ. Geol. Surv. Kans., I, pp. 140-144, 1896. ¢ Jour. Geol., vii, pp. 857-374. Stratigraphy of Kansas Permian—Beede and Sellards. 87 creek the Wreford limestone is exposed. The interval be- tween this outcrop and the base of the Florence flint, in the Crusher quarry is 61 feet, barometrically. This interval represents the thickness of the Matfield formation at this locality, with, perhaps, some of the upper part of the Wre- ford limestone. (For the description and definition of the formational terms used in this paper see the two papers of Prosser previously cited and Folio 109, U. S. Geol. Surv. Atlas. It is also necessary to: call attention to Adams’ paper, Bull. 211 U. S. Geol. Surv., 1903, in which these formations were discussed and given the names pro- posed by Prosser in the latter of the two papers referred to which appeared about 10 months prior to Adams’ paper. Consequently Adams’ statements concerning the Elmdale, Eskridge, Matfield and Doyle formations, pp. 54-59, that “It has not heretofore received a distinct name” etc. etc. are in error. More lamentably so because from his own statement to me he was thoroughly cognizant of Prosser’s paper for months before his paper was published.—Beede.) Owing to an anticlinal structure north of the Kansas line the Wreford limestone appears at the B. and M. R. R. junction as just mentioned and is somewhat fossiliferous. The section beneath the U. P. bridge is as follows: Ae nert. a, fourteen ineh layer !.. 202. send cae se 1 ft. 2 inches: 3. Limestone, irregular and rather thin bedded...... Se ee AT) os eS ALC Sear ATG WUds ads) ene, cietoheiave S Siac: oSecyslaie le oi slaveyerove Se gk Oe 1. Shales, blue, extending to the creek bed.......... Ze eee Mes ANDHEM LY 6. apenas peeuenics Cae neta (anes ay eae ae 9 ft. 2 inches Numbers 3 and 4 probably represent the upper part of the Wreford limestone and are somewhat fossiliferous while 1 and 2 are probably interbedded shales with the major part of the limestone below. At Holmesville (not visited by the writers) a little over 20 feet of limestone, according to Knight’s section may be referred to the Wreford, the lower six feet of which is cherty.* The section at the state line was not visited by the writers but according to Knight’s section there are 35 feet of Matfield shales, numbers 1 and 2 of his section,* and apparently 15 feet of Florence flint, number 3. . However it seems probable that number 4 of his section contains about two feet of cherty limestone belonging to the Flor- * Op. cit. p. 363. + Loe. cit. p. 367. 88 The American Geologist. ADEVstTAeUe ence flint. Numbers 4 to 7 represent the Fort Riley lime- stone, of which 33+ feet are shown in the section. In Beede’s section at Oketot the top of the Matfield is shown in the ravine just north of the depot. The thickness of the Florence flint is given as 17 feet and the total thickness of the overlying Fort Riley limestone is given as 37 feet. Passing down the Big Blue river to Marysville we find the same general conditions repeated. In the northern part of the town 11 feet of the top of the Matfield forma- ~tion followed by 20 feet of the Florence flint and 26 feet of the Fort Riley limestone are exposed, as shown in the fol- lowing section: _ MARYSVILLE SECTION. 10. Limestone, thin bedded, disintegrated ........ 2+ ft. 0 inches 9. Limestone, brownish with fragments of pelecy- DOGS. Bajo ecictcetarele aeiereie inte ater Oe Bleneraseteie Oe oe tees 8. Limestone, thin bedded, light colored grading INTO -SNAlC)vrccstonstevs cies ieisicrore eetered «wise ate-aketorets BY amet! Yet 7. Limestone, cellular, with iron streaks and stem- Tike pmMarksr at el ee ees att si wove evaten tates eke Uh LM AO aes G:: .Woimestone;s cellular =i yae cserstever oh aos levees seyoreneroree By Ste eee 5. Marls and clayey shales with brachiopods and DFYVOZOANS . < O.,s.. Gah ae 29. Limestone, shaly: and shales! 227. ssscmeleen 3 Oe iO ka ies Qs Shales reds ercen and volivies asses eee eens a. 3 Gees ae snales mealcarcouse. se os +. AA SOS RAR RENE Sr Lee Oe 26; “Shalessrred) and) yellow . ii odessa ose ea cee mec 3) es Zire AIM ESTON CG. warss Kaito. bas Gus cokoustonewe Bust arebeeae eae aids OV. 1 Ge ee 24 SasS alegre incre Wa saad te: ot as cee oie 4 o> ee Zo eeuIMestone ands SHALES! ceiere aie eonle ac eis iace 2 1G ames QAO Siee co ie car ortioletnicn vor totetnict re oie a tia thoroor nae 2, es Onna 21. Shales, indurated; and limestone ............ iL ‘OG rh Bers 205 MShaics lchtrcolored) S2hias-eoe cone clteloe eae Art ta S ee OP Ree 19 SS eeimestone ss OptO s,s. Siee cc enckepo srokecers: shee tes ierever helms Se 0 4 “e ee Shales lieht-sred dish) syecuscotieneciee er eerie Ap SS Gian ae lic sLimestone.slapby. osinchatonens rei ceracreccicen 1 ae) * 16" - Shales; reddish *iias terion aon soccer 7 mice a V2 15: * Limestone: sMmassiview nests oer on eee ae Lt) SEO es BA LCOVEREA yo se eis ee eee he Sas gee ene aera mare mee Bi eee OME dae 13:, Flint and limestone” ...%.6.... eae ae ree Oe en ae uIP O10 (2) o10 ears era aie ais Gh GR OO ao ao Un oo dole AI iw oc” eae ae If. Shales maroon sand (Sree locee a. om oes ee Bee: SA eee 10. Limestones with green shale partings....... Dt ee SOY ae te 9; ;Shales Seen te wees pees ester his ei olen keds stee oicne’ sterehs Oates iO eens 8. AZIMESTONE MST ai facts oer atoudeneie Sesto ea laeeneel Os Satie eS ee Ge. “shales. bright: /2Teenirce.n.ncisiciens «cetereie oes Ctenetelre a SSR Ones OS TuiMeStOMe! eee er uc tevemapererchcmeus icveiere tere cenis 2 poe 0 eae” 5. Clay and shales, lower % cross bedded and DlOCKY. . ARR eee ay ites Ate bie e Or” EO eae 4. Conglomerate with calcareous cement, fish COS tH ll in ChetOnmo cia erie cicatolocieeelsrarsleraiers OLemes ever Ades o Clay. with) smooth jomts +4 ocr selec ene ee Oe POS ea49 se 2. Shales, blue, green and maroon, indurated.... 4 KN) a 1. Shales, reddish, lower part covered, high water TEI) fs sigh Rea Ae Peete etal rc ova BR ie eerie Se BESO mae TOG: aaiis.cs0:5)0oo SRO eee ore ke aCe 210 ~=aft. 0 inches This gives 29 feet of the Garrison formation in this exposure with probably 23 feet to be added as Hay’s sec- tion gives 25 feet as the thickness of the Wreford at this locality. It is very probable that number 13 of our section is the top of the Wreford. The thickness of the Matfield formation here is 48 feet (52 feet according to Hay). The Florence flint is 22% feet (given as 25 to 30 feet by Hay). If number 29 were added to the Florence flint it would cor- Stratigraphy of Kansas Permian---Beede and Sellards. 95 respond to Hay’s section, but would reduce the thickness of the Matfield formation an equal amount. Numbers 31 to 37 of our section are Fort Riley limestone and show a thickness of at least 47% feet of it exposed, with the prob- ability that much of Number 38 should be added. The region from Junction City to Cottonwood Falls has been well summarized by Prosser.* Taking the region as a whole he ascribes a thickness of 6 feet to the Cotton- wood limestone, 140 to 145 feet to the Garrison formation, 40 feet to the Wreford limestone, 60 to 70 feet to the Mat- field formation, 20 feet to the Florence flint, 40 feet to the Fort Riley limestone, 60 feet to the Doyle shales and 20 to 25 feet to the Winfield limestone. Detailed sections are given in the folio referred to. Southern Province.—South of the region represented in the Cottonwood Falls folio changes are to be noted in the appearance of some of the strata under consideration. South of the latitude of Bazaar, Chase Co., the Cottonwood lime- stone has never been definitely located nor its horizon accu- rately mapped. Keyes? states, referring to the Cottonwood limestone, that “its geographic range is wide, extending from Nebraska through central Kansas into Oklahoma.” Again? “The stratum (Cottonwood limestone) has been traced from southeastern Nebraska where it passes beneath the Cretaceous, entirely across Kansas into Oklahoma. It often forms a noticeable topographic feature.”’ The Cotton- wood limestone has never been traced across Kansas into Oklahoma unless it was done by Keyes himself. Indeed, as will be shown in the following discussion, it can not be recognized with certainty by any of its characters south of the region just mentioned. Other stratigraphic changes occur in the Garrison, Eimdale and intermediate formations so that the members can not be recognized readily by their lithologic characters and can only be determined by care- fully tracing the outcrops south from the known localities. One of the writers endeavored to locate the Cottonwood limestone in the southwest corner of Lyon county and tra- versed its general horizon to Reece but was unable to locate * Jour. Geol., iii, p. 773 and some of the preceeding pages. See also Cottonwood Falls Folio, U. S. Geol. Surv. Atlas, number 109. + Amer. Geol, xxiii, 1899, p. 308. ¢ Loe. cit. p. 311 96 The American Geologist. August, 1905 it with certainty. At Reece, Beaumont and Grand Summit excellent exposures of all the important limestones of the entire section are shown, but nowhere is a stone with all the characters of the Cottonwood limestone to be found. The fauna of the general horizon is somewhat similar to that of the Florena shales but it is distributed through a fairly wide range of rocks and is nowhere so pronounced as in the northern localities. In short the Cottonwood limestone ceases to be of great value as a horizon marker south of the latitude of Bazaar. The stratigraphy of this region can best be compared with that farther north by detailed sections. The regions near Reece, Beaumont and Grand Summit furnish excellent exposures of the rocks concerned in the Flint Hills escarp- ment. North of this region the flints have been so con- stantly associated with this escarpment that it has led to some errors of observation in its southern prolongation. For this reason the sections near the places just named are given in considerable detail. SECTION FROM REECE TO SUMMIT SIDING. 70. Limestone, massive with many chert concre- CONS “IN AVES! sic. o siccieciacss shes shoe these sus 15+ ft. 0 inches 69. Limestone, very cherty, covered with fallen CRETE occa iscacs Seared eee rele ala esate ie ete koe Se ee Ue 68. Limestone containing 3 or 4 layers of flint. Pusulinas: c/s honckk cree dure acsuoeehesic o eonecareoe Sh cade tpacs 67. Tsimestone:ashallvareceryce a cecil cisie corals oorices 3° Le Omics 66; sShalesScalcarcousseennceni cao ee ota Oy Sais Be 654 limestone, (shally: eer sien sem ccna shoe cen a oe Lh Soe Ones 64; Shales; blue, -caleaneouSieserss o.. sclociewieciaerntee Ae eed ee ote 63. sbimestone:; shally he er icre bears eitaredare eee 2 tes (Re 62. Shales, yellowish and greenish ............. fo ee Olas Gi). (COVETE) traslos cee IIs 3:3 ek I eeons Sie rete One res 605" Limestone; hard? massive see: . seca s 32) E280) See 59s) }Shales:ssfossiliferousm sc. eeeeeeee ere Bi ATE Oe a 58. Limestone, rotten, and fossiliferous.......... Does 0, ee 57. Shales, yellowish, indurated, fossiliferous.... 9 “ 0 “ 56. Limestone, rotten, and calcareous shales.... 3 “ 0 “ 5b. =Shales)) green) ‘and? yellowishis.. scence oe ste Bee SG) = oss bas Shales se maroon acs cscs cis staid eke eevee bee oan (1) Pee 53; Shales) brishtsreen: fi... cieeccerperroreerereieie tele tetere Qe eR re ‘Stratigraphy ot Kansas Permian---Beede and Sellards. 97 bueeeiamMestone,, Massive, Nard’ -< . ts «isis efete ese oe geet a PETHESTONEH SHOAL: ors a0 oa dames —-Shates;-green and bite sort ies ear SEO eae Sie 90s 1. Limestone, brown;omassive! with) Produetus)'io, esisd2 5 Yeora [ i §} Bs r Ly los SESe Peveciasterene atatrne See ee 2003880 feats dtichas 0) vdd snoteomit- .vEé Nigh ene TI to -3-are-in- etre ere west! of thie road juat northwest. Of: “REcEe the remaining lower’ part’ cot the: sec= tion (numbers 45t9.9) extends, up; the bluif, Trom’t the creek, Numbers 10 to 21 are ingthe; cuts: near, the spring, about 134, milés west of Reece on the rathwadh« escarpinent bad ‘been filledjoas had: the snialler ones between it and the érest’of the rrdger ‘Tt Seéuring the material for the fills “the available Séil and ‘loose ‘material had. been remeved from the right of way, in the, vicinity of, the cuts, leaving ideal,exposures: from: whieh to. make, exact sections. “These a threw *hght om points! swhichi were béfore obséuré! * hi the Vight of our ‘sections’ we ee the following’ summary of formations. auOS TSS ape Names: 1,to 40, are.Coal Measures. Or i amalepaml et * Kank. Unive Quart.,- vi, p. 158, footnote. aLiaaot Stratigraphy of KansassPermian“Beedé and Sellards. 64 hot ibeif/gcabletorrecognizethe formations with certainty 94 thiMlowerpareof the sectidaritds deeineddbest’ not te at! tempectoidrawe approximate lines to! the formations, though thesé numbers includecthecequivalents’ ofthe” Elmdaly NevinoEskridges Cotton woolliandoGarrison® formations 2atid probably sormdé ofthe formations bélow.2° Numbers“4t to 32 aresthe: Wa ord dimestond with a thickness of'over'27 feet Scinchesiw Fhe dMatfield fortiationis reptesented-by at tease s8-fedvi6 inches of récle) avithout nimber' 67, which woutd make it 62 feet 2 inches, (numbers 53! (itd 67ypr0 There ts mote sordess4oPdiqikStionks to whether or not’ number 67 should besclassediawivh’ the! 'Matfieldo’ We arecindlined 3 inebudétit:with theeFlopencé Mint!’ Numbers 67, or 68, 86°76 representithé Fidretce fifto witha thickriéss -of! 21° fee 6 inches: Withoutsmumb er! 67 10r!lasnfeet-a aches! with dee7sd9 oft A large atotntef plantiréihains wastaken* from d! cu? in theowagbioroad just east of d! sinalloravine Heat the! 4p bf the escarpthent! westiof Reeeeo!oThis horizoh seemed *d be cthe née quivalentsof | Wwumbers°1G’an@'20, though this Cowra hot déterniaied!avith? dértainty: (dt is Probably2 WélP Gowt int thee Bimdale dormutidn possibly! dt itsbase.oo Numbeirgs producédw latgevanimberlafo plant remains, fish atvd osttal eods! he! Cottohwood limestone was not’ located with certainty and as a consequence the thickness of the Garret sdftiiformation: Canctict be! statedo> Tposeers' probable that Proser’s Ibeation ofthe horizon of the: Cottonwo6d time stone is approximately correct) He’ locates it ‘as ‘probably being in nember 7 Gr /696fChisSeéetion? which is nearethé top! of Number: 22 bf ourcséction.» Prosser refers numbers rprs of fis séetibn to! the Wreford Hmestone* giving: Tt! a thickness of 50 feet. In looking6Ver his notes previous’ to writing .this,paper ,it-wasp discovered that;in passing over the section twice his baronretersgave different readings for the covered portion.of the,section, between the, two, flints and in) compiling: the section the)ismatler, reading: was used. This was alsozinvaéeofdance with the! general appearance of the’ Section. ‘Even 1 with the sides Stripped as they, were thickness of the strata ‘exposed between the upper cuts by Rane Univ. Quart, Ji, «Py 12. Strong | ‘Aint 2 Wretord nihestonel a 100. The American Geologist. August, 1905 walking along the railroad. The upper part of the Wreford limestone was partially concealed as was most of the Mat- field formation. Number 13 of Prosser’s section corres- ponds to numbers 41 to 45 of our section. Number 14 of his section corresponds to numbers 46 to 47 of our section, including the shales and upper limestones of the Wreford limestone and all of the Matfield formation. The remain- der of our section, numbers 68 to 70, corresponds with num- ber 15 of his section, and represents the exposed thickness, of the Florence flint. From the foregoing it is clear that the Florence flint forms the crest of the “Flint Hills” west of Reece. From there west to El Dorado the railroad passes down the dip- slope of this stream. Proceeding south from _ Reece, changes vegin to appear in the rocks making up the front of the escarpment. The Florence flint falls back to the west forming another small escarpment west of the town of Beaumont and the Wreford limestone has been removed from the notch through which the railroad passes in cross- ing the ridge, though it appears on the crest just north and south of Beaumont. The Wreford limestone outcrops in the streets of Beaumont, somewhat below the crest of the ridge east of the town which is formed by rocks of lower horizon.* South of the Reece section the “Frisco” railroad climbs the escarpment with numerous cuttings which produce practically a continuous exposure. No attempt was made to go to the base of the escarpment to establish a section but a base was chosen about 200 feet below the Wreford limestone, possibly in the top of the Elmdale formation. The detailed section follows: SECTION OF THE “FLINT HILLS” ESCARPMENT EAST OF BEAUMONT. 42. Covered, to the base of the Wreford limestone in the crest of the hill south of 'the railroad 20 ft. 0 inches 41.° Shales, red and blue, disintegrated, showing IM GUE Biikaoe ick See eae cake menos s+ * 0 vy 40. Shale, indurated, blue calcareous. ........... 5 soe tos 3 “ce 6 “ce 39. Shale, calcareous disintegrated .............. + This correction also applies to the section published in U. S. Geol. Surv. Folio 109, p. 3, column 3. * Sellards left the field at the close of the work at Reece. Stratigraphy of Kansas Permian---Beede and Sellards. 101 38. Limestone, massive, fine chert concretions in COD ae ee reereve cre akat at-this, section’ is itt the approximateohdrizbniof bathe voCatténwoddohmestone, judgin® fron? its- general: fee es i ne & elie ier, 9p02 a section and numbe shdy Cares 2a, Pau 2 A, to, gestiom should: prove to be correct the hickinestiabetleehteeees rison formiatién at. this. locality. wouldbeo4 46efeet2!si% SS Tif two Streams heading on the cregt/6F the Hd aera removed the ary ete from the ois = the, earaet siniles solittplossBeaamorolhs tell GreabSunt! f mit region fahious: ee fossils. : Fhe logical 2P ety to, this region is) from oth north ‘v where. t en) eaumont, section, furnishes a valuable e key. ee, “Conditions.herei: wolsde .8f This section, will:be-eonsiderad im two» partsatizentGrandr Summit, 6r lower,.section and. the -CambridgéBulen, or upper, Section. The detaifed SeetidhH of the Grahd Stiinmit, if if fotloy, gi iyo avotvetq to sesd of dlatwolloy ,esisde .0 WS” ky sy sai iit 20 aay yIsde ,notesmid .e [ (ie a _ GRAND SUMMIT. SECTION. oo tdsil .zolsda .8 29. “Shattes,” blue, . with. caleareous: sheets ‘and: mil---- bere ved a 28. * ) pe: 6625 sagertth a 27. Shales, mines fetes @bove® cen eves 5 . OmOTepmtiedd .F 26. “Shates ‘and shaly. limestone2hogelsdge9, bas ebgqyoelsq@ « 25. Limestone, setndwhats massive, Swedtiwalia’ omolacmil 6 pew | di hiaae te eat matters mrt nano ctr sean uicicle cle elle geliz2zog§ « i” 24. “Shafes,’caléareous, and impure. limest6fé 802 Joule setae 23. Shales, clayey, with calcareous layer, very fos- Stratigraphy of Kagsxs-Permian-Beede and Sellards. 103 inicsilifenousc.oc. sve. bas-idel.bos-2soree. vir Hon sadT Pfhns EABABIABC: Seta (Modular sand clay;shales. 3}. 25553450 ie ie Some fo fo ssils BT. aigios Sat SvOdE s54t GG 3 ce = ae 21 Sh ales, yeflow and blue with caleareous lenses. - =a 03 3? tu ehing ee. bbs blac da pcr te TE as EN tees 5 feet baie gib sit. inplioen. Jignmmco bret NO MS HANES TCO! 2 oye cc's sce sore, ccs 6.0, 0. 5DS872- bsoulesd sof @ isiips ted bHesd blue, coe berderee) te eae pom] 4 * blue, mas ive a ae Seteiecus te mt ay al nesione, ef1i5se J ft 52 Sih INSIW WO TO As ik ‘gts ‘3 yellow an red, 1 foot of lim m eeone Fa 6 aa HEMT pe ERE phée 221727, 282 Bt redaid olyyl s.ogo a 3 eR oie kaver! 10. 2igvs!. grot« ia s¢orii 14s 2Shalespyelowish, calcareois-esan9is:. dea bient 59 40 z2bed 13,7; Limestone, Shaly cn 3/- -unjor ff: edt: to -esend logs n s foi 2, Sha ee eR ak alas ‘ ‘ol 4gs3 1doikO tk woof to teow Hormsup sgote 4 Gushi “x0 2 ‘two “thy OHeRo ee ete eked By aaa = 18 Shates O78! Snosésinit biotot IT aglt Yo apsduocs 9, Tbmmyéstonés buff to browniste large? Fisalinas >» s bszoqxs vi no .bsrhnd chert; inyithe: lewer!-parts; -sclt.30. noite Mods vhtis} Arofbeles AaveR|;; tls srft tocdtnour sdt io ters bent +Soo“ sd: ails dod vite Ff ign tg mae W052 Siiwollot sil tlt 2 orld ee ve ee aT eee S20s3 glirw squeoqxs 410 Limestohe, mabsive, initwadayers.sc3. acals. Sgbtidens to Sri Shales; yeHowish, iwith calcareous) layers rieh ++ flo) sonst 2 heeded eee sitooxs ‘s18 pipe SH lig yeoris inofiqisces 2. Limestone, dark colored, in thin levers ‘full to) pelkac}pod’ OT. SNCIAGMAD MOAX.“OITOSS SHD 1. Shales, red and blue, in creek north of the cut, east” SP He treba Weer PRE ARITO [O° zorion! ‘eree ddyts DASE EM ye LD Dae te Be 1 JUD TODA 10.M0H ji9sdD. “ef ey ie eee a a oi jr9do ditw ,ovieesor ,»a0j290 ait i! as » . va } e frotal °1.,.2m0isstom09 J1sdo avotsmun a: a = 2 5 2 io) ) a a 7 oO oo 3 4 © a 5 by - oe = | 32 — Ee HH: S OEGIE ie) my m3 |: B20) 6 Tom ditw mwysl feeto po visde There, aré : somewhere. é fro om ,90 to 125 f¢ ocks | 5 in the. hills togthe ngrth of Grand SEEM rane be.addeg, to this (section, but they. are better. exposedicinihes sections _ whith #& t6 follow. ..Phe Wreford limestone caps: tHeistisp off the hill§ north of Grand Summit and is in the Ae ridge West of towp. . .Thg. most conspicuous Featre GF the Wretord. limestope herg is the greatpblocks.of semisilicified dimestonec apparently formed by. infiltration: oWd iscdseanthanaeter off this” lirfestoné throughout edtsdsouthier 9p uexténtasetohiorés pronouficed hére-than farther north. °'PAeReMDIEK Se Heth e# out brown and the farmers use them to fill mud-holes in the road, build fences, &c., calling them “sandstones.” 104 The American Geologist. Angnet eee They are very porous and light and have the smooth joint surfaces of chert. The top of the hill west of Grand Sum- mit registered 90 feet above the town. ‘Taking the dip into consideration this would add more than go feet to the Grand Summit section. The dip to the west is probably equal to the railroad grade. The limestone quarried at Cambridge may be number 25 of our Grand Summit section, but it seems probable that it is one a little higher in the series. At Grand Summit ‘there are four layers of limestone with intervening shale beds of considerable thickness, between the top of our sec- tion and the base of the Wreford limestone. The lime- stone quarried west of town at Cambridge is 94 feet below the base of the Wreford limestone. The latter is excellent- ly exposed across the creek south of the quarry, where a fairly good section of the underlying rocks is to be had, on the point just east of the mouth of the little tributary from the south. The following section is a compilation of this exposure with those from the old Torrence station, just west of Cambridge, along the railroad to Burden. From Tor- rence (old station at the Creek) to Burden at the top of the escarpment almost all the strata are excellently exposed. THE SECTION FROM CAMBRIDGE TO BURDEN. 39. Chert concretions and weathered limestone, topvof-Burdenscuteeeen os eee echee lone 2+ ft. 0 inches 38. Limestone, massive, with chert in layers..... Oe 0 aed 37. - Limestone with numerous chert concretions..10 “ 0 “ 36. Shaly calcareous layer with some fossils...... Bo Se she OF gee oe 35. Limestone, shaly, full of pelecypods.......... Oi neces a ah 34." Shales) ‘dark redand blue’ <2). 2222 a0: 2s. i ieaeas van 9: 334: “Shales; DlUish?=. sje cies 6 ce eee 3 Halted ue (Voy: Sen -Bluish ;marl...scitacicsee Gee « one coma ee el oto 31.,..Shale. reds a. chr. wea sees oe eee 4. St 0 Faeese 30: Limestone, ‘shaly below +o. nmece- «ce deci OF eae eT Oh. ote 29. Covered ..... a ela Lavelle S Sao aR ere ooo releere cae 20%" ee 0 ee 28. Shale, bluish, and calcareous nodules........ One 6E Se 27. Massive limestone, two layers .............. BS) “SP Gee ae 26. Limestone, impure, shaly; shales on top....:.2 “ 0 “ 0 “é 26.. Shales, blue:and olive i2ccou- secrete « oS Stratigraph iy of Kansas Permian—Beede and Sellards. 105 24. Limestone, massive, mottled and Touch... Shoe UN aes: 23. Limestone with three thick layers of chert... 3 “ 0 “ ME OVELCG chien nso chatecysiatelc. oo eketel nr at snore s eiciae. ema attra Se mae Oe ee DACEEOLIVCUS AICS ts eteicrs lors lererciere ets c. ci ole soe ois siete cio shes i eee | ae 20a shale; yellow, arenaceOus | .02:.642%)cis2 eee ee 1 Oe 19. Limestone, massive, chert in top............. a my Pe eT ple ee 18. Limestone with large chert concretions...... Gree) Ob ses 17. Limestone, partially silicified and carrying GHET res ics wrens che 20s Hie Oo ORI oC Tea Ge oc 16. Limestone with coarse chert concretions....:4 “ 6 “ 15. Limestone full of small chert concretions..... GWie hae Le 14. Shales, calcareous and impure limestones, LOAVES? 0 ob Gog und A DOOD LOe DOR OOUMOnUOe ries 0 alll alee COLA VAN ALC Sime ore ictevs scacake 6. she Geb ae Sualersneiels oie $. opc.0rs O-faae OR AES Te, “SUM DIGEE SHES b coe 6c Gcipine ¢ OK oLEiO OoUO ERO IOC ION Oni Bat AOR ars elem CO ONGLC GE ary oA = 0. os falas, Sei eiepa orsaoe's eS ale. see-dse's tinal oA O CR TOle bAmestone,, TOULN; MASSIVE... 6.0... cceeles eee 3 ee Oeics Mii eR LO Siar yr vatirees: oie > pie cy cinievebene ei cpotio, 6:0) Siteigs st asec Snsidvans Sig So Gi ies Saeemestone: TOSsiliferouUs «. 0220). . & 9f'avea At {10 DSiW i OM 2 eee Tf DS KOI fi 4. TO 2x9D071 i i I = 5 f a : ere rH 59Fr OorKehi wo arsjeow of jsdi o1ussisstl 5d3 mort tasbivs af iT” -2U19 “wdevorods Isinomsbout s 2i saoxttA to J1sq 10(sm sdj ai bas bsblot bas bolsantos vistsotitat teom Yo guaitel2znoo .xsiqaroo onillst q .039 .2tetio2 orbasidgaiod bas evososolat .adeetiones .2931asTs f J I OF oni — i it 2 x8 J eos 29 ,2Iniog » x5iquiroo 2i stave ) d5 169 ) i he > Tso to ipo siow ¢ 229507! 9b snr & of resd oved Hos yK ait 9if Gz 09 2ids 3 off Bet 19t91 fio od B ateido 9 7 f sfT52 S13 | i yidw ) h 8 {imo tsqqs 2i o194d3 I anw 2 ) 19 t 112 The American Geologist. Amguat; 2988 THE FUNDAMENTAL COMPLEX BEYOND THE SOUTHERN END OF THE ROCKY MOUNTAINS. By CHARLES R. KEYES, Socorro, New. MEX. ‘Soon after passing the southern boundary of Colorado the Rocky mountains rapidly dwindle and disappear as a pitching anticline beneath the plains of the Mexican table- land. In this limited New Mexican area the Archean, or Azoic, rocks form the cores of several of the principal ranges. The last exposure of the fundamental complex is in the Apache canyon, which the Atchison, Topeka and Santa Fe railway makes use of in crossing the mountains. South of this locality the only exposures of ancient crystallines are in the great fault-scarps of the block mountains, which rise out of the plains, forming the general surface of the Mexican tableland and the NeW Mexican portion of the High Plateau region. During recent years many facts have been brought to light which have very radically modified opinion regarding the great crystalline basement underlying all the Paleozoic sequence in New Mexico. Most of the extensive formations composed of granites, schists, and gneisses which form the axial foundations of so many of the mountain ranges of the region are now believed to be of much later geological age than is generally understood to be covered by the title, Azoic or Archean. In summing up our knowledge on the subject, a decade ago, in his paper, the Pre-Cambrian Rocks of North Amer- ica, Van Hise* remarked: “Tt is evident from the literature that in western New Mexico and in the major part of Arizona is a fundamental, thoroughly crys- talline complex, consisting of most intricately mingled and folded granites, gneisses, micaceous and hornblendic schists, ete., precisely as in the previous sections concerned with the Rocky mountain system. This complex occurs at many points, constitutes the axes of many ranges, and its structure is of so intricate a character that no attempt has been made to estimate its thickness or to work out its structure, although in general the laminated rocks have been referred to as metamorphic. The granite in this complex plays the same part with reference to the crystalline schists as in the other areas referred to. Besides this ancient granite, which existed be- fore the next newer series of rocks was formed, there is apparently * Bull. U. S. Geol. Surv., No. 86, p. 331, 1892. The Fundamental Complex---Keyes. 113 in certain areas granites of later age, and these are more plentiful as the western part of Arizona is reached.” In the light of the recent discoveries that in some of the mountain ranges of New Mexico portions at least of the crystalline foundation are of clastic origin, it becomes neces- sary to devise criteria by which the crystallines of the fun- damental complex (Archzan) may be separated from those that have a sedimentary origin. Until the application of these criteria to every mountain range is made, no general deductions can be drawn concerning the exact ages of the different crystalline formations. The reasons for this state- ment are obvious from even a casual examination of the basal crystallines in New Mexico. It is known that in all of the New Mexican mountains where the crystalline base- ment is open to view a marked unconformity exists at the base of the fossiliferous sequence. The late Carboniferous limestones generally rest directly upon the granites, gneisses and schists, the foliation of which is more or less steeply in- clined or even vertical. That the erosion interval represented by the uncon- fo1mity was very long is quite evident. In southern New Mexico the early Carboniferous limestones begin to make their. appearance. Then come Devonian beds, Silurian or Ordovician, and finally what appear to be Cambrian. A horizon of great unconformity persists under all the Pale- Ozoics. Something of real significance of the old erosion plain becomes manifest by reference to the geological section dis- played in the Grand Canyon of northwestern Arizona to- wards the western border of the High Plateau region. The author* just quoted describes the following general condi- tions: “The Tonto sandstone of the Grand Canyon region, called by Powell and Gilbert Silurian in accordance with the nomenclature of the time, by present classification is to be placed as Upper Cam- brian. The great unconformity which separates this sandstone from the earlier series makes it very probable that the latter are pre- Cambrian. These inferior series in descending order are the Chuar, Grand Canyon, Vishnu series (together the equivalents of Powell’s 1 W0Cs Cit., “D:. 33. ~ 114 The American Geologist. mabe Grand canyon group), and the basal complex. The upper series consists of shales and limestones. Below this, with an erosion in- terval, is the second, consisting of sandstones, with interbedded and cutting basic eruptives. Inferior to this series, and separated by a great unconformity, is a set of thinly bedded and nearly vertical quartzites of undetermined thickness, broken by intrusive masses of granite. These three are clearly clastic series. The basal com- plex as described by Powell and Gilbert consists of thoroughly crys- talline hornblendic and micaceous schists, gneisses, and granites, like the fundamental complex of the remainder of New Mexico and Arizona. Between this basal complex and _ the Vishnu series, as shown by Powell, is a vast unconformity. We have then in this region passing from the base upward, a fundamental complex; great unconformity; quartzite series of unknown thickness (Vish- nu); great unconformity; Grand Canyon series; minor unconform- ity; Chuar series; great unconformity; Cambrian.” There are then recognizable in the Grand Canyon part of the region at least four great unconformities in the space between the undoubted fundamental complex of Archean age and the Cambrian sandstones. Each of these four un- conformities represents a long period of time when the rocks were elevated above the sea, flexed and then subjected to enormous denudation. Powell* has estimated that in the case of the latest of the intervals mentioned which is repre- sented at the base of the Cambrian sandstones, at least 10,000 feet of beds were bowed up, contorted and eroded in such a manner as to leave but fragments in the synclinals. Each of the great unconformities represents similar con- ditions. In New Mexico these four periods of enormous erosion were probably superimposed. The clastics of the Proterozoic must have suffered tremendously. Over very large areas every vestige must have been removed. In all likelihood only scattered remnants remained. Thus in ad- joining mountain ranges the crystalline basement may be of— Archean age in the one case, while in the cther it may be Proterozoic. The differentiation of the fundamental Azoic complex from the Proterozoic crystallines must rest upon the appli- cation of some such scheme of critical criteria as has been so successfully formulated in the Lake Superior region. While there is as yet much uncertainty regarding the +. S. Geog. and Geol. Sur. Terr, 1876. The Fundamental Complex --Keyes. IIS position and geological age of the basal crystallines in many of the different mountain ranges there are some instances in which there exists but small doubt as to their Azoic posi- tion. The general proofs are in a measure comparative. They are the relative amount of metamorphism evidenced, the character of the deformation apparent, the difference in petrographical features, the geological relationships, the ab- sence of all evidences of clastic origin, and a comparison with similar features of known areas in other parts of the country. The literature relating to New Mexican Azoic forma- tions refers all the basal crystallines to the Archean. Lit- tle of definite value therefore can be gleaned grom the wide- ly scattered published descriptions of local phenomena. The first suggestion that any portion of the ancient crystallines occurring within the boundaries of New Mexico were any other than of Archzan age is believed to be a recent state- ment regarding the significance of the recent identification of certain ‘“‘quartz-reefs” in the Sandia mountains as highly metamorphosed sandstones.* The present surface exposure of the great crystalline basement underlying all the fossilferous strata in New Mex- ico is relatively small. Aside from the area in the south- ern Rocky mountains in the northern part of New Mexico the exposures of pre-Cambrian rocks are confined almost to linear outcrops found along the immense fault-scarps of the block mountains. Some of these outcropping faces indicate that the rocks are of undoubted Azoic or Archean age, while others are manifestly of clastic nature and thus belong to the Proterozoic. In order to understand more fully this apparent anoma- lous distribution it is necessary to refer to some of the gen- eral conditions prevailing in neighboring states that the geological history discloses. The conception is that the upper surface of the ancient crystalline basement in this region represents an old peneplane on which, when submer- gence took place in Proterozoic times, an enormous thick- ness of sedimentaries was laid down. This whole country, still in pre-Cambrian times, was folded up into mountain * Eng. and Mining Jour. vol. Ixxvi, p. 967, 1908. 116 The American Geologist. August, 2202 ranges, not once, but repeatedly. Finally before the Cam- brian strata of the region were deposited the entire country, already profoundly folded, faulted and cut frequently by in- trusives was planed down to a prodigious extent. On this new peneplane only isolated patches of the clastic rocks of Proterozoic age survived—only those portions caught in the lowest parts of complex troughs, the bottom of synclinoria. These remnants of the Proterozoic sedimentaries now ap- pear so intensely metomorphosed that they have until quite recently entirely escaped notice. At best it is only with the greatest difficulty that the rocks of the two great ages can be differentiated. ; In many of the mountain ranges the crystalline base- ment is composed partially or entirely of gray or red gran- ites which show little or no evidences of shearing or sub- jection to great oroganic pressure. It has been customary to regard these masses as composed of Archean granite. Now granites of this description, practically unaltered, are known to traverse or be intimately associated with the undoubted Proterozoic crystallines. On the principles involved in the separation of unfossiliferous geological formations accord- ing to the relative amount of deformation and comparative degree of metamorphism, these unaltered granitic masses are tentatively referred to the Proterozoic, though for con- venience in treatment some of them probably have to be considered for, the present in connection with the other rock-masses in which they occur. At some risk, perhaps, in the present state of our knowledge, of swinging too far in the direction opposite to that heretofore generally accepted, it seems most advan- tageous to proceed on this hypothesis. In support of this position there are many other reasons which should be fully discussed in connection with the detailed descriptions of the Proterozoic crystallines. For the present only those crys- talline rock-masses will be considered as belonging to the Archean fundamental complex, that consist of much sheared granites, crumpled gneisses and schistose rocks not associated with undoubted clastics. Probably the main reason for the lack of definite and discriminating information regarding the pre-Cambrian The Fundamental Complex---Keyes. 117 rocks of southwestern United States has been the compara- tively limited exposures. Another factor has been that the examination of the formations has been an incidental object in connection with hurried expeditions undertaken for other than geological purposes. In New Mexico the exposures of the pre-Cambrian crystalline basement are for the most part linear in character. There are in this region a score of prominent mountain ranges in which the basal crystallines are exposed to view. At least in half of this number the rocks are with but small doubt of Azoic age. Several ranges present crystallines which are of undoubted clastic origin. In the remainder the age of the crystallines is not definitely known. Most of the ranges will have to be studied anew in the light of the more modern conceptions rendering pdssible the differentiation of the old crystallines into well defined geo- logical formations. In the southern Rockies, which extend down from Colorado less than a third of the distance to the southern boundary of New Mexico, there are four large areas'of basal crystallines all of which, until undoubted clastics are discovered in them, may be considered as com- posed of Azoic formations. As a whole the ranges which collectively go to make up the southern extremity of the Rockies are generally known as the Snowy mountains or the Sangre de Cristo ranges. As the four areas of Azoic rocks mentioned are more or less distinctly separated from one an- other, they will be here taken up briefly in turn. The largest and most important area of ancient crystal- lines occurring in New Mexico is the one entering from the north from Colorado. Comprised within the area are the two important ranges, Culebra, and Taos, which are almost wholly made up of old crystallines. The principal rocks are hornblendic schists, biotitic schists, gneisses, gneissoid gran- ites and coarse-grained unmodified granites. |Stevenson* frequently mentions in this and neighboring districts the existence of beds of quartzite in the granitic and gneissic rocks. Whether or not all of these “beds” are really quartz- itic clastics cannot now be told. From what is personally _ known of the character of the rocks generally in this region *U. S. Geog. Sur. W. 100 Merid., vol. iii, Supp., p. 68, 1881. 118 The American Geologist. we A sc it is not believed that any of them are of clastic origin. Some of them are certainly aplitic; and others are known to be quartz-veins inclined at low angles. According to the writer just mentioned, the rocks im- mediately north of the boundary line in Colorado are pre- dominantly hornblendic schists, though there are some mica schists present. These schists occupy the middle and high- est portions of the axis. On the east side of the range gneisses and gneissoid granites prevail, together with some mica schists. A coarse-grained granite is also frequently met with. Southward, within the limits of New Mexico, the horn- blendic schists become less and less prominent. At the boundary line the Azoic belt is not more than 6 or 7 miles in width, but within a short distance it rapidly broadens out to 20 miles. The prevailing rocks are dark and light colored gneisses, some bands of the latter very closely resembling beds of quartzite. Occasionally bodies of coarse-grained ‘granites are met with. 3ordering the front of the Rockies, from a point near the northern boundary of New Mexico and extending south- ward a distance of over 30 miles, is a rugged ridge known as the Cimarron range. These mountains are composed largely of Tertiary eruptives. Where the range is deeply cut by canyons which traverse it, as for example on the Rayado, the Cimarron, and several branches of the Vermejo, Azoic rocks are disclosed beneath the spread-out eruptives. These old crystallines are chiefly light colored micaceous schists and dark hued fine-grained gneisses. Occasionally these rocks are broken through by coarse-grained red granites. ’ In-the southern part of the range the base of crystal- lines is covered by basalt flows from the great Ocate crater, which rises out of the plains a few miles to the southeast- ward. The areal distribution and the structural relationships of the Azoic basement in the southern part of the Cimarron range are at present somewhat obscure. The apparent irre- gularities in the distribution of these rocks is probably due largely to the presence of the Mora arch which extends in a The Fundamental Complex---Keyes. 119 northwesterly and southeasterly direction through the Turkey mountains. The genesis of this arch is probably of quite recent date. It crosses the great fault that runs along the eastern front of the Rockies which late erosion has greatly obscused at this point. The Azoic core of the Las Vegas and Mora ranges forms a narrow belt which begins a few miles north of the crossing of the Pecos river by the Atchison, Topeka and Santa Fe railroad and extends northward a‘distance of 65 miles. It is bordered on each side by wide belts of Carboni- ferous limestone. The most prominent peak is Solitario, which rises to a hight of 10,260 feet above sea-level. At the northern extremity, the rocks appear to be al- most entirely hornblende schists. A few miles to the south- ward light colored micaceous schists and gneisses are the prevailing rocks, with some dark colored gneisses occupy- ing the central portion of the belt. At Mora the principal rock is a gneissic granite, while farther on appear again the micaceous schists. From the Cebolla canyon the gneisses and schists appear to be profoundly affected by deformation agencies. From Solitario peak southward the predominant rock is a coarse-grained granite with occasional bands of gneiss. _ The east side of the Rio Grande valley in northern New Mexico is bordered by the lofty Santa Fe mountain range, the highest peak of which, known as Baldy, is 12,660 feet above the sea-level. The central axis of this range is com- uosed of ancient crystallines bordered on each side by Car- boniferous rocks. The crystalline belt is 50 miles long, by 6 to 8 wide in the broadest place. At the southern end in the Apache canyon the prevailing rock is a red granite. Granite bands and masses appear at frequent intervals far- ther north in the gneisses and micaceous schists. In the Santa Fe canyon there occur in the gneiss bands of argilla- ceous slate. Farther north the rocks present similar geolo- gical characters. Archean granites are reported by Stevenson as com- posing the Placer (Ortiz) mountains, 20 miles south of San- ta Fe. No granite is found in these mountains. The rocks are micaceous and augitic andesites of laccolithic origin, 120 The American Geologist. Bapasty 1 OUb and probably of early Tertiary age. The same is true of the neighboring Los Cerrillos hills, the Cerro Pelon, the Tuertos group, and the San Ysidro. if Thirty miles west of the Rio Grande, and about the same distance north of the city of Albuquerque are the Na- cimiento and Jemez mountains. The first mentioned of these is a block mountain 20 miles long. Along the great fault scarp, and under the Carboniferous limestones form- ing the backslope, the basal crystallines are well exposed. These appear to be chiefly granites, so far as observation goes. Their age is as yet undetermined. They are for the present referred to the Azoic. Near the continental divide west of Albuquerque is lo- cated the Zuni dome, its top eroded off down to the crystal- line basement. The age of the pre-Carboniferous crystal- lines is presumably Azoic. As early as 1856 Marcou* men- tions a belt of crystallines in the heart of the Zuni range 12 miles wide, consisting of reddish granite, gneiss and schist. Blake* also calls attention to the gneisses and granites of this district, and corroborates Marcou’s observations. In Dutton’s? account of the Zuni plateau the presence of gneisses or schists is not mentioned. The granites are call- ed Archean. If, however, the observations recorded are correctly interpreted some of the granites are certainly of much later intrusion. This author states that they have metamorphosed the overlying Carboniferous limestones, and calls particular attention to this phenomenon as it is well displayed in Mt. Sedgwick, the most prominent feature in the field. The remarkable mountain blocks known as Sierras Os- cura and San Andreas are over 100 miles long and extend northward from the Organ mountains north of El Paso. The fault-scarps of the two ridges face each other at their proximate extremities, a flat valley lying between the two. Herrick* mentions the granitic character of the crystallines beneath, the the Carboniferous limestones, which dip in op- posite directions in the two ranges. The age and lithologic * Pac. OR. Rs pur VO iia pe liOyelooo: +iPac. R. R. Sur:., vol. iiljop: 38; 1856: +U. S. Geol. Sur., 6th. Ann. Rept., p. 158, 1886. * Bull. N. M. Univ., vol. ii, Fasicle No. 3, p. 5, 1900. The Fundamental Complex---Keyes. 121 character of the crystalline basement are presumably sim1- lar to those of the Organ mountains, immediately to the south, which have in fact a genetic relationship to the San Andreas range. While properly a continuation of the San Andreas and the Franklin mountains to the south the Organs belong to a distinct block which has been elevated much more than any other portion of the long ridge to which they belong. In consequence the sedimentary rocks have been entirely re- moved except at the very base on the west side. The rocks of the Organ mountains are chiefly red and gray, coarse-grained granites. Associated with these are hornblendic and micaceous schists, which are traversed by numerous dikes, which are quartzose, dioritic and andesitic in character. Proterozoic quartzites and clay slates are well developed a few miles to the south, in Texas, and it is probable that these also extend into New Mexico. Ac- cording to Walcott the thickness of the pre-Cambrian clastic section is over 3,000 feet. In Perry’s notes* on the geology of the Mexican boundary mention is made of the granites underlying the Carboniferous limestone of Franklin mountain north of El Paso_and in the Organ mountains, but no specific refer- ence is made to their age. G. B. Shumard?* passed through the Organ mountains in 1857 and noted on the east side hornblende and mica schists, and red and gray granites, all of which were cut by dikes of quartz, greenstone and porphyry. Thirty miles west of the San Andreas range the Ca- ballos mguntains rise abruptly above the Rio Grande valley. These form a block mountain in which the crystalline base- ment is exposed for a vertical distance of 1,500 feet. Biotitic schists, gray crumpled gneisses, and granites form the principal rocks. The granites are of two principal kinds. One, which is more closely identified with the gneisses, is gray, rather fine-grained and contains a large amount of quartz. The other is a coarse-grained, red granite, which appears to be a late intrusive, though it does not penetrate * United States & Mexican Bound. Sur., vol. i, pl. ii, vp. 8. 1857. = + Jour. Geol. Obs. Texas and New Mexico, in 1855-6, p. 113, Austin, 1886. 122 The American Geologist. wets e the overlying Carboniferous limestones. So far as has been observed there are no evidences of the existence of clastic rocks associated with these gneisses. In the Santa Rita mountains, in Grant county, the basal crystallines underlying the Paleozoic limestones are com- posed chiefly of schists. The exposures are small, and lit- tle detailed information on the subject is at present avail- able. The great Mogollon uplift in western New Mexico ap- pears to have an extensive foundation of ancient crystal- lines. The region is so covered by late eruptives that most of the former exposures are covered up. The same con- ditions prevail in the neighboring parts of Arizona. Reagan* appears to have found evidences of the presence of both Archean and Proterozoic formations. The rocks of Azoic age consist of micaceous, talcose, chloritic, and hornblendic schists, and some granites. REVIEW OF RECENT GEOLOGICAL LITERA TURE. The Two Islands, and what came ot them. Tuomas Conpon, pp. 211, pls. 30. Portland, Oregon, J. K. Gill Company, 1902, $1.50. While the author of this volume attempts to supply a popular rather than a scientific want, yet the treatment of the geology of Oregon is thoroughly scientific. The author is a well known geolo- gist who has alone represented Oregon in geological work and geological literature for a life-time. In his declining years he has gathered together the leading facts, discovered mainly by himself, and has in this book preserved them to science, and to the credit of his own labors. He has a large collection of Oregon vertebrate fossils, and he has supplied others to eastern paleontologists. The writer has known of his vigorous activity since the days of his earliest geological work. The two islands described are named Shoshone and Siskiyou, the former in the northeastern part of the state,, in the region of the Blue mountains and the latter in the southwestern corner, ex- tending into northern California, occupying what is now the Sis- * American Geologist, vol. xxxii, pp. 267-308, 1903. . Review of Recent Geological Literature. 123 kiyou mountain region. The author traces the development of these islands into Oregon, and notes the changes of animal life as the development progresses. These islands each had a nucleus as early as the Triassic; they expanded through the Jurassic and had con- tinuous increase in area through the Cretaceous. The Cretaceous was closed by an important geologic and geo- graphic event, the upfold of a colossal sea dyke. This dyke grew into the Cascade and Sierra Nevada range. It separated these islands, the Shoshone being enclosed on the east and thence for- ward associated with fresh water, and the Siskiyou on the west left still subject to marine conditions. This gave the islands different life histories, that of the Shoshone being characterized by land animals whose remains were washed into the lake in which the island stood, and that of the Siskiyou by beautifully preserved Eocene marine fossils. The Miocene was introduced by the slow initiation of the Coast range uplift, forming finally a Coast range: valley between the Cascades and the Coast range which is trace- able from southern California to Queen Charlotte’s sound though having different names in its various parts—the San Joaquin, Sac- ramento, Willamette, Puget Sound. The fresh waters on the east side of the Cascade uplift were gradually reduced in area, from lakes connected by streams to broad low valleys through which single streams flowed. These in- land lakes laid the foundation for the drainage southward of the Colorado river, and that northward of the Columbia river. The Eocene climate was that of the palm and of the rhinoceros, moist and warm. The elevation and continuity of the Cascade range were: not then sufficient to exclude the warm moist atmosphere of the Pacific. Much of the present area of Alaska, as pointed out by the author, was yet under the ocean, and there was presented an open passage for the Japan current, flowing eastward on its way to the Hudson bay and the coast of Greenland, thus “cutting off all accu- mulations of ice between Oregon and the Arctic ocean.’ These subtropical conditions were gradually changed to more temperate,- and even Arctic, by the increasing elevation of the Cascades and the exclusion of the Japan current. This change was-accompanied by the loss of the rhinoceros and the palm tree, the introduction of Miocene animals and plants and finally the Pliocene. At the close of the Eocene the Shoshone island was joined to the eastern mainland. The larger mammals then swarmed over the island. These were Oreodon, Rhinoceros, Entilodon, Bothrolabis, various small rodents, cats like the cougar, dogs, diminutive horses having three hoofs instead of a single hoof, the composite genus Anchitherium With the introduction of the Pliocene the Miocene strata were slowly and unevenly elevated, the Miocene lakes were drained and large quantities of igneous rock were thrust upward through great orifices in the strata. The Pliocene lakes were smaller and their 124 The American Geologist. August, 1905 sediments are marked by two characteristic fossils which run through them all, the camel and the horse. The horse was of numerous forms, the most noteworthy being Hipparion and Proto- hippus.. The camel was in two groups, the camel proper and the Anchenia, the former perhaps as large as the Arabian camel and the latter about the size of a goat. Fossil remains of the real horse, indicating an animal about as large as a good sized dray horse of to-day have also been found in the Pliocene and were described by Prof. Condon in 1866, the earliest in North America. The author divides the Pliocene of Oregon into two groups, the Dalles and the Silver Lake groups and gives notes of their verte- brate remains. It is in the latter that he found, associated with remains of camel and other Pliocene fossils, obsidian arrow points indicating that man lived in Pliocene time in Oregon. Prof. Cope accepted that conclusion, but Prof. Condon supposes that the case is not proven, since the human implements may have reached their position by simple gravitation through the denudation of some thick- ness of Pliocene strata which originally may have separated them from the camel bones. The existence of sand dunes in the imme- diate vicinity, suggesting powerful winds, and the fact that the bones and the arrow heads are mixed promiscuously on the bare surface, give some shadow of plausibility to this supposition. But it is plainly necessary to subject the region to an extensive and more detailed survey before it will be possible to pronounce positive- ly on this question. Prima facie the evidence points as Cope con- cluded, but owing to the importance of the conclusion it may be best to hold it in abeyance. ; The “surface deposits” are those that have accumulated since Pliocene time, bogs, swamps and-all slight depressions in which large mammals often sink to their death. They are Pleistocene and contain the remains of mammoth, mastodon, the broad-faced ox and the sloth-like Mylodon. ‘A large part of this geological period over- laps that of prehistoric man.” Up to the Glacial period the horse and the camel were abundant in Oregon and their continuance through Glacial times is still in doubt. The author devotes a chapter to “The Willamette Sound.” This body of water covered the Willamette valley and was connected with the Pacific. It was an incident of recent changes of level along the coast of Oregon and Washington. The sediments are thick, nicely stratified and in some places contain great numbers of fossils of recent shells mostly identical with those now living along the shore. The waters of this sound rose to at least 350 feet higher, relative to the land, than the Pacific ocean of to-day, and they buried the whole region under a fine loess which reaches the thickness of over 100 feet and forms the present soil and subsoil of the valley. The author does not indicate what may have been the chronological relation of this sound to the Pleistocene, or to any part of it. No human remains have yet been found in its sediments. Review of Recent Geologica! Literature 125 The latest geological event seems to have been the rise of the land to its present attitude, accompanied perhaps by volcanic activity in some of the peaks of the region. The book is a very useful compend. It would have been im- proved by an index and still more by an outline map of Oregon. On the map could have been expressed various localities which the unfamiliar reader would have referred to eagerly, and it might also have shown some geological data. Nic Be Ww. Ice or Water: Another Appeal to Induction from the Scholastic Methods of Modern Geology. By Sir Henry H. Howorru. In two volumes. Vol. I, pp. liii, 536; Vol. II, pp. viii, 498. Long- mans, Green and Co., London, New -York, and Bombay, 1905. In these controversial volumes, published a few months ago, Sir Henry Howorth returns with redoubled zeal to his warfare against the glacialists. All extant or even obsolete theories of the causes of the Ice age are reviewed and analyzed. Weighed in the author’s balance, they all are found wanting; none seems to him accordant with sound physical principles, and competent to explain continental glaciation. Therefore, in his judgment, the Ice age, in which the glacialists believe, must be a myth, merely a figment of their imagination. To follow this destructive criticism, however, a constructive third volume is promised, completing the series thus entitled, which last volume will be devoted to exposition of the author’s theory of the origin of the drift by the agency of rushing waters or floods, the renowned debacles of geologic science two or three generations ago. From his early studies and publications, “A History of the Mongols,” and “Chingiz Khan and his Ancestors,’ which led our author through central and northern Asia, he first came forward to challenge glacial doctrines in a memoir most amply illustrated by Siberia. This was “The Mammoth and the Flood, an Attempt to Confront the Theory of Uniformity with the Facts of Recent Geology” (pages xxxii, 464; London, 1887). Six years later, he again assaulted these doctrines of glaciation, imputing them to wild imagination, such as gives affrighting dreams, in “The Glacial Nightmare and the Flood, a Second Appeal to Com- mon Sense from the Extravagance of Some Recent Geology” (two volumes, pp. xxviii, 376, and xi, 377-920; London, 1893). In a con- siderable degree the new volumes cover the same ground and use the same arguments as that former work; but the present discus- sions and adverse criticism are more elaborate, with large polemic additions, brushing aside and toppling down, according to the auther’s opinion, all the ingenious devices by which the followers of Agassiz have sought to account for the climatic conditions of their Glacial period. In opposition to the epeirogenic theory, which seems to the reviewer to be true and sufficient to explain the accumulation of 126 The American Geologist. Aerial A Pleistocene ice sheets, Sir Henry refuses its most important evi- dence and support by his denial that the fjords are valleys of river erosion. To his mind the great depths of the fjords beneath the sea level are not a proof of former high land elevation, because he regards these very deep meandering and branching valleys as fis- Sures produced by rock fracture! But geologists can not give cred- ence to this view of the origin of fjords, nor can they go back a century to the diluvial theory of the origin of till, moraines, and glacial striation. W. Uz. The Rocks of Tristan d’Acunha, brought back by H. M. S. ‘Odin’, 1904, with their Bearing on the Question of the Permanence of Ocean Basins. By Pror. Ernest H. L ScHwarz, Rhodes Uni- versity College, Grahamstown, South Africa. Transactions of the South African Philosophical Society, vol. xvi, pp. 9-51, with two maps and a section; May, 1905. It is held by this author, following Judd and Suess, that the interior of the earth is composed of a heavy metallic center and is covered by an envelope of siliceous slag. Where volcanic action reaches up from very great depths, it would therefore be expected to bring great masses of metallic substances, like the nickeliferous iron of Ovifak in Greenland. But in no instance has an oceanic island of volcanic rocks yielded a mine of any metal. Nearly every- where the seat of volcanic upflow appears to be of relatively small depth, where the motion and friction of bending and shearing along great fissure lines have melted parts of the sedimentary or older crystalline rocks of the earth crust. On the lofty island of Tristan d’ Acunha, and on numerous other Jone voleanic islands of the South Atlantic, fragments of granite, gneiss, or other rocks of continental types, have been found, lead- ing to the hypothesis that formerly a continental land mass occu- pied that area, which is now enveloped by profound oceanic waters. The ancient land is supposed to have reached from Cape San Roque to Sierra Leone, on the north, and from southern Brazil through Tristan d’ Acunha, to the Cape of Good Hope, on the south; and it is conjectured to have existed from Devonian to Late Tertiary times. W. U. Geological Survey of New Jersey, Annual Report for the Year 1904. Henry B. KummMet, State Geologist. Pages ix, 317; with 19 plates and 18 figures in the text. Trenton, N. J., 1905. Besides his administrative report, the state geologist writes of the molding sands and the mining industry. The production of iron ore from the New Jersey mines in 1904 was nearly half a million tons, being greater than in any former year since 1891; and the zine ore production was 250,025 tons. Dr. Charles R. Eastman presents a report on the Triassic fishes of New Jersey, noting sixteen species. Stuart Weller describes the fauna of the Cliffwood clays in the Raritan formation, and classifies the Upper Cretaceous formations and faunas of the state. Review of Recent Geological Literature. 127 F. B. Peck treats of the tale deposits of Phillipsburg, N. J., and Easton, Pa.; and Arthur C. Spencer reports the progress of work in the Pre-Cambrian rocks. Ww. U. The Geology of the Perry Basin in Southeastern Maine. By GEORGE Otis SmitH and Davip Wuite. U. S. Geol. Survey, Professional Paper No. 35. Pages 107, with 6 plates. 1905. The earliest report of Dr. Charles T. Jackson on the geology ,of Maine, in 1837, recommended boring for discovery of coal in the sandstone formation bordering the west side of Passamaquoddy bay, in the vicinity of Perry, that formation being supposed to be a continuation of the bituminous cnal series of New Brunswick. Later, on the evidence of fossil plants, the Perry beds were regarded by W. B. Rogers, Newberry, C. H. Hitchcock, J. W. Dawson, and others, as of upper Devonian age, being thus older than any known rocks containing commercially workable coal. But citizens of that district, deeming the question yet undecided, petitioned the state legislature two years ago for an appropriation to be expended in drilling for coal, which led to the special survey reported in this paper. The Perry formation is found to comprise, in ascending order, a lower conglomerate, a lower lava, an upper sandstone, and an upper lava. There has been no very marked folding and but slight alteration of the beds; and their age is shown to be distinctly upper Devonian, and probably Chemung. It is certain that they contain no workable coal deposits. Ww. U. ¢ MONTHLY AUTHOR’S CATALOGUE OF AMERICAN GEOLOGICAL LITERATURE ARRANGED ALPHABETICALLY. AMI, H. M. Memorial or Sketch of the Life of the late Dr. A. R. C. Selwyn. (Trans. Roy. Soc. Can. See. Ser., vol. 10, Sec. 4, pp. 173-205, 1904). AMI, H. M. Bibliography of Canadian Geology and Paleontology for the year 1903. (Trans. Roy. Soc. Can. See. Ser., vol. 10, Sec. 4, pp. 207-219, 1904). AMI, H. M. Preliminary lists of Fossil Organic Remains from the Potsdam, Beckmantown (Calciferous), Chazy, Black River, Trenton, Utica, and Pleistocene formations comprised within the Perth Sheet (No. 119) in Eastern Ontario. (Reprint from Ann. Rep. Geol. Sur. Can., vol. 14, pp. 80-89, 1905.) 128 The American Geologist nee ARNOLD, RALPH. Gold Placers of the Coast of Washington. (U. S. G. S. Bull. No. 260, pp. 154-158, 1905). : BAIN, H. FOSTER. The Fluorspar Deposits of Southern Illinois. (U.S. G. S. Bull. No. 255, pp. 71, Pls. 6, 1905). BAIN, H. F. (and E. O. ULRICH). The Copper Deposits of Missouri. |U. S. G. S. Bull. No. 260, pp. 233-236, 1905). BAIN, H. F. Lead and Zine resources of the United States. (U.S. G. 5S. Bull. No. 260, pp. 251-274, 1905). BEAUCHAMP, WM. M. Perch Lake Mounds, with Notes on other New York Mounds. (Bull. New York State Mus., pp. 77, Pls. 12, 1905). BECKER, GEO. F. Simultaneous Joints. (Eng. Min. Jour., vol. 79, p. 1182, June, 1905). BERRY, E. W. Fossil Grasses and Sedges. (Am. Nat., vol. 39, p. 345, June 1905). BOUTWELL, J. M. Progress report on Park City mining district, Utah. (U. S. G. S. Bull. No. 260, pp. 150-154, 1905). BOUTWELL, J. M. Ore Deposits of Bingham, Utah. (Eng. Min. Jour., vol. 79, p- 1176, June, 1905). BOUTWELL, J. M. Vanadium and Uranium in southeastern Utah. (U. S. G. S. Bull. No. 260, p. 200, 1905). BOWMAN, ISAIAH. Pre-Pleistocene Deposits at Third Cliff, Massachusetts. (Science, vol. 21, p. 9938, June 30, 1905). BOWNOCKER, J. A. The Salt Deposits of Northeastern Ohio. (Am. Geol., vol. 35, p. 370, June, 1905). BRADY, F. W. The White Sands of New Mexico. (Mines and Minerals, vol. 25, p. 529, June, 1905). CROSBY, W. O. Genetic and Structural Relations of the Igneous Rocks of the Lower Neponset Valley, Massachusetts. [I.] (Am. Geol., vol. 36, pp. 34-47, July, 1905.) Monthly Author’s Catalogue. 129 CUSHMAN, J. A. Fossil Crabs of the Gay Head Miocene. (Am. Nat., vol. 39, p. 381, June, 1905). DILLER, J. S. Mineral Resources of the Indian Valley region, California. (U. S. G. S. Bull. No. 260, pp. 45-50, 1905). EGKEE EC. Iron and Manganese Ores of the United States. (U. §S. G. S. Bull. No. 260, pp. 317-821, 1905). d ECKEL, ECG. Cement Materials and Industry of the United States. (U. SC ssesiinesNOneate, PDs oto, Pls. 15, 1905). ELDRIDGE, GEO. H. Asphalt and Bituminous Rock Deposits of the United States. 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Zine and Lead deposits of southwestern Wisconsin. (U. S. G. S. Bull. No. 260, pp. 304-311, 1905). 130 The American Geologist. August, LOU _GRATON, L. C. The Carolina Tin Belt. (U. S. G. S. Bull. No. 260, pp. 188-196, 1905). GRATON, L. C. (see HESS, F. L.) GROVER, N. C. (and J. C. HOYT). Report of Progress of Stream Measurements for the Calendar Year 1904. (Wat. Sup. & Irr. Pap. No. 126, pp. 127, Pls. 2, 1905). HARRIS, G. D. (and A. C. VEATCH). Report on the Underground Waters of Louisiana. (Bull. No. 1, Geols Surs Was, pps 64s RIsaSs 905): HAY, 0: P: The Fossil Turtles of the Bridger Basin. (Am. Geol., vol. 35, pp. 327-342, June, 1905). HAYES, C. W. ayes seen of Iron aoe Nonmetalliferous Minerals. (U. S. G. S. Bull. No. 260, pp. 28-32, 1905). HESS, F. L. (and L. C. GRATON). The occurrence and distribution of Tin. (U.S. G. S. Bull. No. 260, pp. 161-188, 1905). HIDDEN, W. E. Results of Late Mineral Research in Llano County, Texas. (Am. Jour. Sci., vol. 19, p. 425, Jume, 1905). HILE, ROBT. 7. Pelé-and the Evolution of the Windward Archipelago. (Bull. Geol. Soc. Am., vol. 16, pp. 248-288, Pls. 43-47, May, 1905). HITCHCOCK, C. H. The Geology of Littleton, New FEampshire. (Reprint from History of Littleton, pp. 32, map, 1905). HOBBS, WM. H. Examples of Joint-Controlled Drainage from Wisconsin and New York. (Jour. Geol., vol. 13, p. 363, May-June, 1905). HOYT, JOHN C. (See Grover, N. C.) IRVING, J. D. Ore Deposits of the Ouray District and in the vicinity of Lake City, Colo. (U. S. G. S. Bull. No. 260, pp. 50-78, 1905). JAMIESON, G. S. Natural Iron-Nickel Alloy. Awaurite. (Am. Jour. Sci., vol. 19, p. 413, June, 1905). JOHNSON, D. W. The Distribution of Fresh-Water Faunas as an Evidence of Drainage Modifications. (Reprint from Science N. S., vol. 21, pp. 588-592, April 14, 1905). Monthly Author's Catalogue. 131 LAMBERT, AVERY E. A Trilobite from Littleton, N. H., with notes on other Fossils 9 from the same locality. (Reprint from History of Littleton, pp. 32- 38, 1905). LEA, SAM. H. The Cement Resources of Alabama. (Mines and Minerals, vol. Zope oole June, 1905). BEE, W: oF: Note on the Glacier of Mount Lyell, California. (Jour. Geol., vol. 13, p. 358, May-June, 1905). : LINDGREN, WALDEMAR. Production of Gold and Silver in the U. S. in 1904. (U.S. G. S. Bull. No. 260, pp. 32-39, 1905). LINDGREN, WALDEMAR (and F. L. RANSOME). The Geological resurvey of the Cripple Creek district, Colo. (U. S. G. S. Bull. No. 260, pp. 85-99, 1905). LOOMIS, F. B. Hyopsodidal of the Wasatch and Wind River Basins. (Am. Jour. Sci., vol. 19, p. 416, June, 1905). MATTHEW, W. D. The Mounted Skeleton of Brontosaurus. (Am. Mus. Jour., vol. 5, p. 638, April, 1905). McCASKEY, H. D. The Mineral Resources of the Philippines. (Eng. Min. Jour. vol. 79, p. 1042, June, 1905). OGILVIE, IDA H. The High Altitude Conoplain. (Am. Geol., vol. 36, p. 27-34, July, 1905). 4 PIRSSON, L. V. Petrographic Province of Central Montana. (Am. Jour. Sci., vol. 20, p. 35, July, 1905). POWER, F. DANVERS. The Gympie Goldfield. (Eng. Min. Jour., vol. 79, p. 1040, June, 1905). RAND, H. W. (and J. L. ULRICH). Posterior Connections of the Lateral Vein of the Skate. (Am. Nat., vol. 39, p. 349, Jume, 1905). RANSOME, F. L. Ore Deposits of the Coeur d’ Alene district. (U.S. G. S. Bull. No. 260, pp. 274-304, 1905). RANSOME, F. L. (See LINDGREN, WALDEMAR). RED. BF: The Variations of Glaciers. IX. (Jour. Geo]., vol. 13, p. 313, May-June, 1905), 132 The American Geologist. ge RUSSELL, I. C. The Pelé Obelisk Once More. (Science, vol. 21, p. 924, June 16, 1905). SARDESON, F. W. A Peeuliar Case of Glacial Erosion. (Jour. Geol., vol. 138, p. 351, May-June, 1905). SCHOCH, E. R. The Genesis of the Tarkwa Banket. (Eng. Min. Jour., vol. 79, p. 1235, June 20, 1905). SCHOLTZ, CARL. The Coal Fields of Arkansas and Indian Territory. (Mining Magazine, vol. 11, p. 520, June, 1905). SCHUCHERT, CHAS. The Nomenclature of Types in Natural History. (Science, vol. 21, p. 899, June 9, 1905). SHERZER, WM. H. Glacial Studies in the Canadian Rockies and Selkirks. (Smith- sonian Miscellaneous Collections, vol. 47, part 4, p. 453, 1905). SMITH, G. O. A Molvdenite deposit in eastern Maine. (U.S. G. S. Bull. No. 260, p. 197, 1905). SMYTH Hive: The Origin and Classification of Placers. I. Il. Ill. (Eng. Min. Jcur., vol. 79,.pp. 1045, 11179, 1228, June, 1905)). SMYTH, C. H. Jr. The Abstraction from the Atmosphere by Iron. (Jour. Geol., vol. 13, p. 319, May-June, 1905). SPURR, J. E. (and G. H. GARREY). Preliminary Report on the ore deposits of the Georgetown mining districts, Colo. (U.S. G. S. Bull. No. 260, pp. 99-121, 1905). SPURR, J. E. The Ores of Goldfield, Nev., and developments at Tonopah during 1904. (U. S. G. S. Bull. No. 260, pp. 132-150,- 1905). TALBOT, M. Revision of the New York Helderbergian Crinoids. (Am. Jour. Sci. voll 20) pr Wee siulys 19. 05)F TARR, RALPH S. Drainage Features of Central New York. (Bull. Geol. Soc. Am., vol. 16, pp. 229-242, pls. 37-42, April, 1905). TARR, RALPH S., Moraines of the Seneca and Cayuga Lake Valleys. (Bull. Geol. Soc. Am., vol. 16, pp. 215-228, pl. 36, April, 1905). Monthly Author’s Catalogue. 133 TARR, RALPH S. The Gorges and Waterfalls of Central New York. (Reprint from Am. Geog. Soc. pp. 20, April, 1905). ! TIGHT, W. G. Clarence Luther Herrick. (Am. Geol., vol. 36, July, 1905). ; TIPTON, J. C. The Cumberland Gap Coalfield. (Eng. Min. Jour., vol. 79, p. 1135, June, 1905). ULRICH, E. O. (See BAIN, H. F.) ULRICH, J. L. (See RAND H. W.) UPHAM, WARREN. Age of the St. Croix Dalles. (Am. Geol., vol. 35, p. 347, June, 1905). VEATCH, A. C. (See HARRIS, G. D.) WARING, G. A. The Pegmatyte Veins of Pala, San Diego County, California. (Am. Geol., vol. 35, p. 356, June, 1905). WEED, W. H. Notes on the gold veins near Great Falls, Md. (U. S. G. S. Bull. No. 260, pp. 128-132, 1905). ; WEED, W. H. Ccpper Production and Deposits of the U. S. (U.S.-G. S. Bull. No. 260, pp. 211-217, 1905). WELLER, STUART. The Fauna of the Cliffwood (N. J.) Clays. (Jour. Geol., vol. 13, p. 324, May-June, 1905). WESTGATE, L. G. The Twin Lakes Glaciated Area, Colorado. (Jour. Geol., vol. 13, p. 285, May-June, 1905). WILLARD, D. E. Agricultural College Survey of North Dakota. Second Biennial Report for 1903-4, pp. 187, pls. 36, 1905. WILLISTON, S. W. The Hallopus, Baptanodon, and Atlantosaurus Beds of Marsh. (Jour. Geol. vol. 18, p. 338, May-June, 1905). WILLISTON, S. W. On the Lansing Man. (Am. Geol., vol. 35, p. 342, June, 1905). WRIGHT, G. FREDERICK. The Ancient Gorge of Hudson River. (Records of the Past, yol. 4, p. 167, June, 1905). 134 The American Geologist. Augast ota PERSONAL AND SCIENTIFIC NEWS, Pror. Ries OF CoRNELL UNINERSITY has been engaged during the summer, on an investigation of the clays and molding sands of the Virginia coastal plain. W.T. McCourt, INstructor In Economic GEOLOGY in Cornell university, has been studying the peat deposits: of New Jersey for the N. J. Geol. Survey. Mr. H. Fosrer Ban is engaged in a study of the Rocky mountain zine fields for the U. S. Geol. Survey. He will visit Colorado, New Mexico and other producing territories to arrange for the collection of statistics of production for the Division of Mineral Resources. PROFESSOR T. C. CHAMBERLIN has been appointed a member of the Illinois Geological Survey Board. The re- maining members are ex-officio, governor Deneen and presr dent James of the State university. Mr. Bartry Wittis returned in July from Europe where he had been since February working under a grant from the Carnegie Institution. Dr. C. W. Hayes of the U. S. Geological Survey spent July and August in Utah and other western states inspect- ing field works Pror. Epwarp Orton JR , State Geologist of Ohio, spent three weeks in July studying the glacial geology of Lowes Peak, Colorado. The remainder of the summer he will spend in Massachusetts engaged in editing one of the bulle- tins of the state survey. Field work for the Geolpgical Survey of Ohio is bee carried on by other members of the survey. Prof. John A. Bownocker is studying and map- ping the Pittsburg ae in eastern Ohio and completing a bulletin on the salt fields and industry of the state. Prof. Charles S. Prosser is studying the Devonian and Carboni- ferous formations of the state and part of the summer will be spent on his report on the stratigraphical geology of these formations. DurRING THE Month oF Jury Mr. M. L. Fuller and F. G Clapp of the United States geological survey made a recon- naissance trip through Newfoundland and along the coast of Labrador to a point north of Hopedale for the purpose of comparing the glacial features with those of northeastern United States. Several interesting points relating to possi- ble pre-Wisconsin deposits, to the origin of the high terraces and to the recentness of the last glaciation, were brought out. The intention was to go further north, but this was impossible because of the presence of unusually heavy pack ice along the shore from which the vessel was obliged to withdraw after penetrating it for a distance of some ten miles. *LOVUVLVO TVIOVTIS) AO ALIS *LSAMHLUON YNIMOOT TANNVHD ATTIIASANV( 0 avaH a ol « "TAM MM a+) NVOINEUNY THE PwPRICAN GEOLOGIST. VOL. XXXVI, SEPTEMBER, 1I905. No. 3. PLEISTOCENE FEATURES IN THE SYRACUSE REGION.* By H L. FAIRCHILD, University of Rochester PLATES VI. AND VII. The district lying near the city of Syracuse is one of unusual interest to the student of glacial and geographic geology. In addition to the common forms of Glacial drift there are here displayed a remarkable series of stream canons arid cataracts cut by the ice-border drainage, and the shore phenomena of Glacial lakes, specially of lake Iro- quois. Moraines are not strongly represented among the drift forms of the region. No heavy or well-defined moraine oc- curs near the city, although some masses of hummocky drift are to be seen. Most of the drift burden of the ice sheet was here built into drumlins. Valley moraines occur far south of the city, as has been noted in the description of the railroad routes. Kames, or water-laid or stratified drift in the form of knolls or mounds of gravel and sand, are scattered over the region, and are conspicuous in the southern part of the city and along the valley sides, their structure being well shown in the excavations for building sand. The remarkable features of the drift known as “drum- lins” are excellently shown in and around the city. The city lies in the eastern end of the belt of drumlins, perhaps the most remarkable in the world, which extends west for a hundred miles. Every hill between Syracuse and Rochester is a drumlin; adthough some of them have a base or core of Salina shale. * Prepared for the field programme of the meeting of Section E, Am. Assoc. Adv. Sci., Syracuse, N. Y., July 19-22, 1905. 130 The American Geologist. September se South of the palallel of Syracuse, which lies at the line of the north-facing escarpment of the Onondaga limestone, the ancient valleys that were cut by north-flowing streams are very prominent, the country being a series of north and south valleys and intervalley ridges, a part of the “finger lakes” area. North of the parallel of Syracuse, and where the strata are mostly a great thickness of soft Salina, Niagara and Medina shales, the valleys have been obliter- ated, partly by the drift filling, and possibly to some extent by the removal by the ice of the saliences in the soft Salina. The city lies in the northern end of the visible Onondaga valley, on a plain produced by Glacial and lake filling. Deep borings for salt show a great depth of valley filling, but the topography of the buried valley can only be determined by systematic borings. In the deeply buried sands of the valley the brines accumulate from the adjacent salt beds, making Syracuse the “saline city.” During the recession of the continental glacier from this region, the ice sheet acted as a barrier to the northward drainage by blocking the northern ends of the valleys. In consequence, lakes were held in all the valleys extending southward into the highland. The earliest and highest waters in each valley found escape southward across the col at the present valley head; but later, as the ice front gave” way, the overflow was across the intervalley ridges past the ice border. The evidences of these ancient waters are the deltas built at various levels by the tributary streams, and the outlet channels which determined the several levels. Some of these channels and correlating deltas are very prominent features. The description and naming of the local lakes in the valleys of the Syracuse region may be found in pages 52-63 of the article: noted) im) the list of weferences, as Nov asses this may not be available to all readers, a brief enumeration of these lakes is given as follows: In the Otisco valley the primitive and highest water, called the Glacial lake Otisco, had its outlet southward over the col. The lower water, the Mariette lake, escaped west to the Skaneateles valley. In the Onondaga valley the highest water was the Cardiff lake, which had its outlet south through the Tully lakes. Later, Pleistocene Features---Fairchild. 137 the waters fell to the hight of the outlets at Joshua and Navarino, leading west to the Otisco valley, and are called the South Onondaga lake. A yet lower lake, the Onondaga Valley lake, had eastward escape by the channels at James- ville. On the Butternut valley the highest lake, Butternut lake, overflowed south across the col and through Tully village, while its successor, the Jamesville lake, had outlet eastward by the channels northeast of Jamesville. The vast expanse of Glacial waters which were held by the waning ice sheet in the Huron, Erie and Ontario basins had their lower escape through the lower members of the local lakes already mentioned. These were the great lake Warren and the lowering waters, of which only one pause had been determined, namely: lake Dana. The Warren waters reached this territory with an altitude of about 890 feet as the present level. The Dana waters were about 180 feet lower, and the outlet of lake Dana is believed to be the great channel leading east from Marcellus.’ The numerals given in connection with the channels shown in the accom panying map, show the present altitude of the heads of the channels. (Plate vii.) . The successor of the Warren water and the falling Warren (Hyper-Iroquois) in the Ontario is lake Iroquois, with its outlet at Rome over the Mohawk valley. Lake Iroquois flooded the Syracuse plain and the lower ends of the Onondaga, Butternut and Limestone valleys. The wave-cut notches on the drumlins and the wave-built spits and bars are to be seen near the city. The most novel and interesting features of the region are the deserted river channels, which were cut by the Glacial waters in their escape to the eastward past the ice border. After the glacier had dumped its rock-rubbish in the valleys and so formed the valley-head moraine, or pres- ent water parting, it wasted away until the ice border was many miles north of the moraines, thus forming the valley basins that held the local Glacial lakes described above, the northern barrier being the ice body itself. The later waters held in these basins escaped across the ridges and pro- duced the fossil channels that are indicated in the map. The reader should clearly understand that the present 138 _ The American Geologist. eptember AP 0s north-flowing streams are in deep and wide pre-Glacial val- leys (these are shown by the topographic sheets), while the extinct channels are cut across the tops of the inter- valley ridges and high above the north-south valleys. In other words, the highest of them have both ends in the air. As the crests of the ridges decline or fall away to the north, the transverse channels on any meridian were cut success- ively from south to north, as the ice barrier receded, and of course at successively lower levels. As no channel was deserted until a lower escape was opened, it follows that each successive or lower channel must have been initiated at an altitude below the bottom of the preceding channel. The Syracuse channels and cataracts were functionally the predecessors of Niagara, as they carried the overflow of western waters eastward to the Ontarian level. Two of the fossil cataracts, those of Jamesville and Blue lakes, are comparable in hight and capacity to the present Niagara. No visitor, standing for the first time on the crest of the Jamesville lake amphitheater and appreciating the romantic history involved in the phenomena, will regret a journey of a thousand miles to view the region. (See plate vi. A brief description of these features, with illustrations, may be found in No. 3 of the references. The rivers which excavated the cross-ridge channels dumped their detritus into the valley lakes. A very prom- inent delta lies two miles south of Marcellus, in the Otisco valley, but this is beyond the easy reach of the excursions. It may be seen on the Skaneateles sheet. The largest delta in the region is in the Onondaga valley at the junction of the Marcellus-Cedarvale channel, and shows on the Tully sheet. It can be reached on the trips and can be plainly seen miles away, from the east side of the Onondaga valley. This great delta extends from a mile northwest of South Onondaga around the north of Indian Village, a stretch of four miles. Another delta lies west of Jamesville at the mouth of the gorge, below the lake and ancient cataract. Still another and more conspicuous delta occurs at High Bridge in the limestone valley at the mouth of the White lake channel, and is mapped in the southeast corner of the Syracuse sheet. Small terraces and benches of stream detri- —$$———_ Geiaieug CO6I 14901039 dIWONOD3 GNY IWIDVID ONIMOHS d¥W HOLIMS i jaLseW| p . svi13q 40 Ke ' SINVNW34 SLVYVLVD WIDVID = STANNYHD TIDv79 S \ ALINIOIA pue Wie . a ay enysor © AN “ASNOVAAS 4 | | cureney © JIVITIASS on x Si7vi Auuvnd Qnois 009 2) |!ASaw er core ao ‘IIA S1V1d ‘IAXXX “I0A ‘LSINOTOUH NYOMANKY pe ~— 9 _— ve Cah tee nates, gs, { if “i ae Ted ; 1 5 at Prin he re ee Sar they To, Oe _— ee —— 5 a Pleistocene Features— Fairchild. 139 tus, built in the Glacial waters, may be seen along the slopes of the valleys, correlating with the lake levels estab- lished by the stronger channels. Those in the Onondaga valley are more specially related to the Railroad channel. REFERENCES, 1. Bulletin Geol. Soc. Am., x: 57-66. Gives a description of the Glacial lakes, with illustrations. 2. Amer. Jour. Sci., vii: 249-263. Describes the Glacial lakes Newberry, Warren and Dana. 3. 20th Ann. Rep. N. Y. State Geologist, 1900, pp. 112-129. Describes and illustrates the extinct channels ard cataracts in the Syracuse region. 4. 2ist Ann. Rep. N. Y. State Geologist, 1901, pp. 33-47. Describes and illustrates the lower channels between Syracuse and Rome, especially the channel which passes through the city of Syracuse. 5. 22nd Ann. Rep. N. Y. State Geologist, 1902, plate 1, facing p. 19. Map with description of lake Warren. 6. Bulletin Geol. Soc. Am., ix: 173-182. Description by E. C. Quereau of the Jamesville lake and surroundings. Car-WInDOW GEOLGGY: SUGGESTIONS TO TRAVELERS. Approaching Syracuse from the west by the New York Central or the West Shore raitlroad,—From Buffalo to Crit- tenden the New York Central R. R. lies on the leveled lake- bottom of Warren waters, the strong beach of which is crossed at Crittenden. From there to beyond Batavia the road is in the well-accentuated Batavia moraine. From there to Rochester the generally smooth plain is diversified with drumlins and low kames. The West Shore road lies on the Warren lake-bottom nearly all the way, and at Smithville station a conspicuous cliff cut by Warren waves may be seen on the south. From Oakfield to Rochester scattered drumlins may be seen on the south. From Oak- field to Rochester scattered drumlins may be seen on the south, with moraine topography at Churchville. From Fairport (east of Rochester) to and beyond Syra- cuse these railroads follow the river channels cut by the Glacial waters in their eastward flow. From Newark east- ward the work of lake Iroquois waves may be seen in numerous notches or terraces on the drumlins, at from 20 to 30 feet above the level of the railroads. For the whole 140 The American Geologist Pepie mabe ahaa distance the drumlins appear in remarkable form. The Salina shales appear in places as red or green clay-like ex- posures, the best display being 3 mjles east of Newark, on the south side of the tracks. Approaching Syracuse from the east by the New York Central.—From Schenectady to Rome the railroad lies in the ancient channel of the Iromohawk river, a stream larger than the St. Lawrence, which carried the overflow of the Glacial lake, lake Iroquois. On the south wall of the valley may be seen the high-level channels cut by Glacial waters when held up by the ice front. Such are conspicuous three or four miles west of Little Falls and east of Utica for sev- eral miles. Between Little Falls and Rome the deltas built in the earlier waters and the flood plains of the Iromohawk are conspicuous. (This stretch is covered by the Utica, Oriskany and Oneida sheets of the geological map of New York State.) From Rome to near Oneida the railroad lies in a pronounced Glacial river channel. All the way from , Oneida to Syracuse the tracks he on the L[roquois lake-bot- tom, while the south banks of the ice-border drainage are conspicuous at many points, on the south side of the train appearing as steep bluffs on the saliences. The north bank of the stream was the ice of the ancient Glacial cap. The West Shore railroad parallels the New York Cen- tral from Oneida to Syracuse and shows the stream-cut bluffs even better, since it les farther south. Approaching Syracuse from the south by the Delaware Lackawanna and Western ratlroad.—Northward from Bing- hamton the road follows valleys which were the southern escape of Glacial waters. The abundant stream detritus may be seen in the broad stretches of gravel plains and in terraces and deltas at the mouths of side valleys. From Tully northward for two miles the road lies in the small channel across the col which was the outlet of the Butternut Glacial lake. From Apulia to Jamesville the road lies high on the west side of the Butternut valley and commands a fine view of the valley features. For three miles north of Apulia the valley is partly filled with moraine drift. Oppo- site Onativia broad delta terraces are seen on the east side, which correlate with the Tully outlet. Moraine drift is Pleistocene Features—Fairchild. I4I conspicuous, either in the valley bottom or banked against the walls. (The Tully sheet covers all this area.) Between Jamesville and Syracuse the road passes through the grandest of the ancient river channels, the “Railroad” channel, which is a fourth of a mile wide and 150 feet deep, mostly in Onondaga limestone. (Syracuse sheet.) Approaching Syracuse from the North —TYhe two branches of the Rome, Watertown and Ogdensburg railroad, and the Oswego division of the Delaware, Lackawanna and Western railroad leading into Syracuse from the north, all lie on the Iroquois lake-bottom but encounter few striking features, though all the ordinary forms of drift appear. At the junc- tion af the two branches of the Rome, Watertown and Ogdensburg at Woodward, the railroad cuts across a heavy ridge or bar of lake Iroquois (Syracuse sheet). From Adams Center south to Richland Junction, more than 20 miles, the R., W. & O. lies on the west (lakeward) side of the heavy Iroquois beach, carrying a “ridge road.” (Pu- laski, Sacketts Harbor and Watertown sheets.) Approaching Syracuse from the west by the Auburn branch of the New Vork Central railroad —At Victor this line is in a great channel of Glacial flow, which it again tra- verses from Clifton Springs through Phelps to near Geneva. At Halfway Station it enters another striking channel, which it follows through Camillus to near Syracuse. This is on the Baldwinsville sheet. 142 The American Geologist. Beptem vere NOTES ON THE PERMIAN FORMATIONS OF KANSAS. By CHARLES S. PRossER, Columbus, Ohio. In 1902 the writer reviewed the recent literature re- garding the correlation of the upper Paleozoic of Kansas with the Russian Permian.* In this review the writer in- advertently omitted reference to the papers of Dr. E. H. Sellards identifying and describing Permian plants from Kansas, although he was familiar with them. In 1900 Dr. Sellards reported the identification of Cadllipteris conferta Sterng. from the Marion formation (or possibly the lower part of the Wellington shales) of Dickinson county in eastern central Kansas and the geological importance of this discovery was discussed as follows by him: “The geological range of Callipteris conferta has an interesting bearing on the question of the age of the uppermost Paleozoic rocks of Kansas. The species is characteristic of the middle and lower Rothliegenden of Europe, but has not been found above the middle of the Permian. It has also been found in the Permo-carboni- ferous of West Virginia. The occurrence of this species near the top of the Kansas strata [in Dickinson county only the Big Blue series or lower Permian occurs; the Cimarron series or upper Per- mian is found farther south] together with Sphenophyllum, a genus that has not been discovered above the middle of the Permian, makes it improbable that the Kansas beds are younger than middle Permian. While, on the other hand, the presence of Callipteris, a Permian genus, and the number and variety of plants belonging to the Tzeniopteroid group, as well as the general character of the flora, tends to confirm the Permian age of the Kansas Upper Pale- ozoic.”’} In 1900 fossil plants were found in the Smoky Hill river valley just east of Salina in Saline county, which ad- joins Dickinson county on the west, in rocks of about the same age as those ofthe former locality. In commenting upon the plants from both of these localities Dr. Sellards Saudi “There are, in the collections so far made, some twenty-six or twenty-seven determinable species, distributed in fourteen genera. The plants indicate unmistakably the true Permian age of the formation in which they are found. Many of the species are charac- teristically Permian, and only a very small proportion of the species identical with Upper Carboniferous species.”* * Jour. Geol., vol. x, pp. 721-787. + Bull. Univ. Kansas, vol. i, No. 2 (Kan. Univ. Quarterly, vol. ix, YOR, 1D) fos EE * Trans. Kansas Acad. Sci., vol. xvii, 1901, p. 209. Permian Formations of Kansas---Prosser. 143 Part of this flora has been described by Dr. Sellards* and in the second paper he identifies and describes Ze@nzop- teris coriacea Goep. which he states: “Seems to have been found as yet in only two other localities, both Permian, Ottendorf in Bohemia, and Lissitz in Moravia.” In 1903 Dr. Keyes published a paper entitled “Some recent aspects of the Permian question in America,’’? in which he objected to certain statements in my article of the previous year. His principal objection, apparently, was that in giving the “Classification of the upper Paleozoic forma- tions of Kansas” the writer used Cragin’s name of Big Blue instead of Keyes’ term Oklahoman for the lower series of the Permian and stated that in Kansas they were identical. The following brief history of these two terms will furnish a basis for judging whether it was a fair statement or not. The term “Big Blue series” was proposed by professor Cragin in March, 18096, for the lower Kansas Permian forma- tions? which he listed as follows: Wellington shales. Geuda salt-measures [which later he withdrew in favor of the name Marion formation]* Chase limestones. Neosho shales.7 Professor Cragin stated that “It may be called the Big Blue series, from the Big Blue river,. which in northern Kansas crosses the somewhat narrowed northern extension of its area of outcrop.”: The upper Permian formations, popularly termed the Red Beds, were named the Cimarron series by professor Cragin in the same article.$ In July, 1896, Dr. Keyes proposed “‘to recognize in the ‘upper’ Carboniferous of the western interior province three series having equal taxonomic rank,” the upper two of which in ascending order were named the Missourian and Oklahoman.* The top of the Cottonwood limestone was + Bull. Univ.. Kansas, vol. i, No. 4 (Kan, Univ. Quarterly, vol. ix, No. 3), 1900, p. 179 and idid. vol. ii, No. 1, (Kan. Univ. Quart., vol. x,. INO: 1); 1901; -p. i: + Am. Geol., vol. xxxii, p. 218. + Col. Coll. Studies, vol. vi, March 27, pp. 3, 5, 6. * Am. Geol., vol. xviii. Aug., 1896 p. 182. + Col. Coll. Studies, vol. vi, p. 3. + Ibid., p. 6. § Loc. cit.. pp. 3, 18. 48; see additional account in Am. Geol., vol. xix, May, 18897, pp. 351-364. * Am. Geol., vol. xviii, p. 25. 144 The American Geologist. Bepiember ae given as the upper limit of the Missourian series and in de- fining the series it was stated that “In suggesting the name Oklahoman as a serial geological term it is intended to apply to all those rocks of Carboniferous age which occur north of the Canadian river in Oklahoma and which lie be- tween the interval of the top of the Missourian series and the base of the Cretaceous. It may be regarded as essentially covering the same succession of strata that has long been vaguely known under the title of ‘Permian.’ The name is derived from the territory in which the formation has its best development and in which the most complete sequence is represented. The best sections across the belt appear to be exhibited along the Cimarron, Arkansas and Kansas rivers, and these sections may be considered typical.’* In October, r901, Dr. Keyes accepted the name Cimar- ron series for the Red Beds? and gave the upper three series of the Carboniferous in ascending order as the Missourian, Oklahoman and Cimarron? stating their respective strati- graphic values as 4, 2 and 1.8 The following month Dr. Keyes published a “General Geological Section of the Carboniferous of the Mississippi Valley,” in which a complete list of the series and terranes of the system is given. For the portion under consideration it is as follows: SERIES, TERRANES.: Cimarron. . cae Kiger shales. Salt Fork shales. | | Carboniferous, | ( Wellington shales. P % : system. Oona eee Marion BETES. 4 } Chase limestone. [Upper | Neosho shales. portion ] : Missourian Cottonwood limestone. | [Upper part] Atchison shales. [ {Wabaunsee of Prosser]* It will be seen from the above quotation that the ter- ranes listed by Dr. Keyes as composing the Oklahoman series are entirely Kansas formations and precisely the same as those given by professor Cragin for the Big Blue series. It was this agreement which led the writer in his “Classifi- * Lota, SD. oi. +Am. Jour. Sci., 4th ser., vol. xii, p. 309. < [bid.. pp. 306, 309. : § [bid., yp. 306. * Am. Geol. vol. xxviii, Nov., 1901, p.’ 502. Permian Formations of Kansas---Prosser. 145 cation of the upper Paleozoic formations of Kansas” to: state that “Tt will be seen that the Oklahoman series, as precisely de- fined above, is identified with the Big Blue series proposed by Dr- Cragin in 1896, and therefore his name, which has priority, is adopted for this classification.” Dr. Keyes in discussing my paper has objected to the above interpretation and made certain statements regard- ing the limits of the Oklahoman series. He says: “When the title Oklahoman was first proposed for the uppermost series of the Carboniferous its upper limits were not very definitely fixed—further than it was stated that ina general way the terrane corresponded to what had previously been called Permian. At that time the Red Beds were regarded as post-Carboniferous in age.’’t The original statement of Dr. Keyes in 1896, when he first defined the Oklahoman series is as follows: “In suggesting the name Oklahoman as a serial geological term it is intended to apply to all those rocks of Carboniferous age which occur north of the Canadian river in Oklahoma and which lie be- tween the interval of the top of the Missourian series and the base of- the Cretaceous. * * * Although there has been little de- tailed study in the’ region regarding the relations of the series under consideration and the Cretaceous above, it is well known that the latter rests in marked unconformity upon all four series of the Carboniferous and at the north extends over still older formations.”* The writer has given a fairly complete historical review of the correlation of the Red Beds or Cimarron series of Kansas? and the following brief statement of the most ‘im- portant changes in their correlation will be of interest in connection with the above quotation. In early papers the Red Beds were frequently cailed Cretaceous and correlated with the Dakota sandstone. In 1887 professor St. John referred them with a query to the Triassic system.t For several years subsequent to this report the age of the Red Beds was generally given as either Triassic or Jura-Trias. In 1893, however, professor Hay changed his correlation of the Red Beds of Kansas to the Upper Permian on account of the discovery of Permian fossils in Texas in beds which he considered as of similar age.* + Jour. Geol., vol. x, 1902, chart opposite p. 718. + Am. Geol.. vol. xxxii, Oct., 1903, p. 219. * Am. Geol., vol. xviii, p. 27. + Univ. Geol. Surv. Kansas, vol. ii, 1897, pp. 75-83. + Fifth Bien. Rept. Kansas State Board Agr., pt. ii, pp. 140, 141. * Highth zéid, pt. ii, pp. 101, 108. 146 The American Geologist. Rertomber ee In March, 1896, professor Cragin named the Red Beds of t\ansas, the Cimarron series, published a detailed account of it. which he unhesitatingly referred to the Permian sys- tem, and subdivided it into ten formations.? It will thus be seen that for some years previous to the proposal of, the Oklahoman series by Dr. Keyes in July, 1896, the Red Beds of Kansas had generally been considered by geologists as belonging in the Jura-Trias, the Triassic or the Permian. It is also evident from Dr. Keyes’ original definition of Oklahoman that for part of the territory he had in mind for its upper limit the base of the true Cretaceous, so that it was an open question whether he intended or not to include in it the Red Beds. It is interesting to note in this connec- tion that in November, 1904, in a “Generalized geological section for New Mexico” Dr. Keyes gave the age of the “Cimarron formation” as Triassic* although Dr. Beede more than three years before had shown conclusively from fossils that in its typical area the greater part of the Cimarron series is of Paleozoic age.* Dr. Keyes in his paper of 1903 indicates the limits of the Oklahoman series in the following manner: “As it now appears, even according to professor Prosser’s pub- lished data, the Oklahoman in central Kansas includes at the base at least one important formation more than the Big Blue series; and at the top at least one formation less. The Oklahoman series in Kansas is delimited above by the top of the Marion limestones. In my various papers, with one exception due to a typographical error arising from inability to see the proof sheets of the article, this fact is clearly indicated. This is particularly emphasized in the memoir frequently quoted by professor Prosser, on the detailed comparison of the Upper Carboniferous of Kansas with the Russian Permian.’’* It has already been shown that the basal formation of the Oklahoman series as defined by Dr. Keyes is the Neosho shale,* which is also the lowest formation of the Big Blue series as defined by Dr. Cragin.? It is, therefore, clear that the basal limit of the Oklahoman and Big Blue series as de- + Col. Coll. Studies, vol. vi, pp. 1-5, 48. * Am. Jour. Sci., 4th ser:, vol: xviii, p. 360) Jour. Geol "vol ix, GJuly,; “901s ps 339! Am. Geol., vol. xxviii, July, 1901, pp. 46, 47. Adv. Bull. First Bien. Rept. Oklahoma Geol. Surv., April, 1902, pp. 1-11. * Am. Geol., vol. xxxii, pp. 219, 220. + Am. Geol., vol. xxviii, 1901, p. 302. + Col Goll; (Studies: < Turbinopsis elevata (?) (Whitf.). ee x Odontofusus medius (Whitf.).... ee x Rostellaria compacta (Whitf.)... < x Bullavconicas (Whitireia fee U ef x Xenophora lapiferens (Whitf.)...| U ss x Lunatia: hallin(Gabb)iisaeeeieitee “1 and 3 x< Calyptraphorvus velatus (Conrad).} U sates | x Atlantic Highlands Cretacic---Prather. 169 Gyrodes infracarinata (Gabb).... bie x< Odontofusus rostellaroides (Whitt) © x Trachytriton atlanticum (Whitf.) . i 4 Modulus lapidosus (?) (Whitf.).. ss x Turritella vertebroides (Morton). g ms Turbinella (?) parva (Gabb).... s x Trematofisus venustus (Whitf.)..| U s x Pyropsis perlata (Conrad)....... £ x Pyropsis reileyi (Whitf.)........ “s x Tudicula plonimarginata (Whitf.) i ~< Pyropsis trochiformis Tuomey).. 2 x Rostellaria svirata (Whitf.)...... a x Pyropsis richardsoni (Tuomey).. id x Gyrodes altispira (Gabb)........ 73 x Rostellites angulatus (Whitf.)... sf x Volutomorpha mucronata (Gabb) ay x Volutomorpha conradi (Gabb).... 4g > Rostellaria nobilis (Whitf.)...... U = 4 Volutoderma ovata (Whitf.)...... oa x< Turritella encrinoides(?) (Morton) a x Gyrodes obtusivolva (Gabb)..... nt »< Rostellites nasutus (Gabb)....... s x Volutomorpha ponderosa (Whitf.) 3 mK Cithara croswickensis (Whitf.).. ss x Pyropsis retifer (?) (Gabb)...... - Se Pyrifusus turritus (Whitf.)...... ‘ x Odontufusus typicus (Whitf.).... of x Rostellites biconicus (Whitf.)....| U Le x Pyropsis corrina (Whitf.)....... sf * Gyrodes petrosa (Morton)........ i x Trachytriton multivaricosum (?) ROU VEENIie her cpertniccve ccc beers curs, ate, 3 o x Rostellaria fusiformis (Whitf.).. + me Rostellaria curta (Whitf.)....... ‘3 x Turritella lippincotti (Whitf.)... og x Turbinella (?) verticalis (Whitf.) e me Pyrifusus multicaensis (Whitf.).. ¢ x Anchura compressa (Whitf.)..... “2 x 2 2 Palecyopods. ma Navesink o|.9 2 ¢ el Sel 21> ra oleol s | o O 'é) Ol & | > Ostrea larva (Lamark)........ Ués& ed1,2&3 M| B Idonearea antrosa (Morton)... 1 wie Idonearca vulgaris (Morton). .| az Ostrea glandiformis (Whitf.).. . U % x XXX Claragella armata (Morton)... Legumen appressum (Conrad) Diceras dactyloids (Whitf.)... Cardium prelongatum (Whitf.) Trigonia mortoni (Whitf.)..... Hxoeyra Costata (SLy)i.. 2s... 4. Veniella conradi (Morton).... Dianchora echinata (Morton).. Neithea quinguecostata (La- TINA), Bess, Shycrstce boicncltiers sacle. ass x Gryphaea vyesicvlaris (Lamark) Hones os < xX X H ) ee eo Nee o. 170 The American Geologist. Veniella subovalis (Conrad). . Lucina smockana (Whitf.).... Lithodomus ripleyana (Gabb). Arca quindecemradiata (Gabb) Inoceramus sagensis (Owen).. Nemodon anfaulensis (Gabb). Nemodon angulatum (Gabb).. Cibota, obesa “(OWhItE)) 2 ec =i Nucula slackiana (Gabb)...... Perrisonata protexta (Conrad) Veniella trigona (Gabb)....... Liopistha protexta (Conrad).. Area transversa (Gabb)...... Bibota uniopsis (Conrad)..... Inoceramus sagansis var quad- THU (OWAohtut))) Gooodaaoosc Inoceramus pro-obliqua (?) GWAhiEED! aceon eroeeiertcc ite Pecten venustus (Morton).... Neithea quinquecostata (lLa- IMATE) Geiotietse sheeiee cietehegs Ostrea tecicosta (Gabb)....... Anonia tellinoides (Morton)... Inoceramus sagensis var vanux- GMS o srte evauere wane eNeV aero sie ge Crassatella rombea (Whitf.)... Ostrea larva var nasuta (Mor- EOI ers err ver cece abasvoraiedstererarste Corbicula. ‘Species? Fae. «.\. cee 1 Panopea dicisa (Conrad)...... Leiopistha inflata (Whitf.).... Pachycardium burlingtonense (WUE) Satie ee eee eels Gnathodon tennidens (Whitf.) Cyprimeria densata (?) (Con- TALC) Srepcisie unre Mermieeverenat wane Cardium multiradiatum (Gabb) Cardium dumosum (Conrad).. Cyprimeria spissa (Conrad).. Crassatella littoralis (Conrad) .| Dosinia gabbi (Whitt.)......-. Crassitella curta (Conrad) (?). Leicpistha pretexta (Conrad). .| Modiola inflata (Whitf.).......| Hxogyra lateralis! 22s... =) EXO vray COStALAMerlerieererderciset Crassatella vadosa (Merton)... Crassatellarispens ce cmieteluseiernere Corbicwlams pos sareiciere iets sersichens MMOGErAMNUS SDS Payetereeveeversloverstek Neithea quinquecostata (La- TL ATKA 4 ee Gi sh case at ete aire tees Veleda tellinoides (?) (Whitf.) Donax: fordim ea) Mars saceiamieicte Leptosolen biplicata (Conrad) Callista delawarensis (Gabb).. Cyprimeria excavata (Morton) Astarte veta (?) (Conrad).... Panopea elliptica (?) (Whitf.) .| Modiola spe cris cyreciteciree stare | Cardita britteni (Whitf.)...... | U U&M U&M U U M U U | | ,2&3 September, 1905 x X XXX xX x x xX X xX XXX x x xX XXX xX Kanon, cw xX XXXXKXXKXX XXX Atlantic Highlands Cretacic—Prather. 171 INimeculana’ SPeCieS So... ces. 5s Dosinia gabbi (Whitf.)....... Crassatclla alta (Conrad)..... U See x Gryphaea (several species)... .| | Navesink | | Crabs claws. (described by H.| Js; AENUIST C1 Pees) 6 MiG BOA Bio } Bed 3 Fish vertebre (large and small).. i Fish teeth (various sizes)...... Sharks teeth (Cestraciont and SOUALOdOMES)) UGieec o clade © he ets x Coprolites (Jifferent kinds)...... x Belemnitella americana (Morton) sae x SiUODEOR MAG AS ee eae ae Boa Wt x Baculites compressus (Say) Mor- OTE teh levee kes anenais, 5. suntahe ne LO} Baculites ovatus (Morton)....... Baculites asper (Say)........... : x Nautilus dekayi (Morton)........ Turrilites pauper (Whitf.)....... ng x Architectonica anncsa (Courad)..| U Heterococeras conradi (Morton) x GIO Oe Gres Rance BAR eES en Bio coe Ae RERe 2 Terebratella plicata (Say)....... OD) hee x EIR OZ OA aa ienelccicus. teushe tans, slerave-s, avesecese 8} x Serpula cretacea (Conrad) (?).. JPllehale peeyenenbatsl C20 ve pom Cleans Caen Gastrochena americana (Gabb)..| M Dentalium subarcuatum (Conrad) Dentalium faleatum (Conrad).... Siliquaria pauperata (Whitf.).... 1 Margaritella abbotti (Gabb)..... i\ IVS UMTS OR sep eyseie cel sis excrerenel sucess 1 Mt. Laurel Sand. Clark gives the Mt. Laurel sand as 5 feet thick at Atlantic Highlands, and includes it with the Navesing and with the Redbank in the Monmouth formation. At Atlantic Highlands it appears as an oxidized zone be- neath the Navesink and is about 5 feet thick. It was traced from Bay View avenue station at Atlantic Highlands in the direction of Hiltons for a distance of 800 feet when it grades into the Marshalltown clay bed and disappears. Bay View Avenue Lens (2). ‘ This is 5 feet wide and 250 feet in length and seems to be part of the Navesink. It is a dark glauconite (see sample C») bed and contains about 8% of quartz grains and the Miscellaneous. Very Common Other Beds Common Very Rare Rare xX x Xx X x x TSS oc:8 x x xX | rz ek The American Geologist. Sento per AEE rest grains of glauconite cemented by clay. No mica flakes noted in this sample. It is a very dark color which may in part be due to the presence of a certain amount of vegetable matter. It lies below the lighter colored green sand of the Navesink (samples C®# and C) and rests above Bay View lens Now3: The Matawan Formation, In the western part of the Atlantic Highlands section the Mt. Laurel sand is underlaid by a quartz sand forma- tion 35 feet thick, which can be traced eastward for 800 feet when it merges into the Marshalltown clay. The Matawan divisions at Atlantic Highlands are in- cluded under Clark’s Hazlet sand or Upper Matawan. The divisions are “Bay View Avenue sand,” (which I have named provisionally, which represents uppermost Hazlet, and may be Knapp’s Wenonah sand). Below this sand, near Bay View avenue, is 30 feet of the dark laminated Marshalltown clay. This latter is 43 feet thick at the eastern end of the section where it has replaced the Bay View Avenue sand. Below this forming the base of the section throughout is the Columbus sand which grades upward into the Marshalltown clay. The Marshalltown clay here is at the top marked by an unconformity. The Matawan beds at Atlantic Highlands are not very fossiliferous, and besides fragments of a crab’s claw there were few fossils obtained from them. From samples examined with the microscope it was shown that the material composing the beds was largely quartz grains both rounded, flattened, and angular, together with some glauconite grains and mica flakes. Also in some samples hornblende, gypsum, pyrite, serpentine, orthoclase, microcline, pyroxene, etc. were found. There is more or less clay with glauconite grains either disseminated or in pockets. The strike is northeast to southwest—dip 25 feet to the mile as given by Clark. Following are the detailed characters of the various members of the Matawan series beginning with the highest. Bay View Avenue Sand, This is so named from Bay View avenue station near Atlantic Highlands where it occurs. It is from 15 feet to Atlantic Highlands Cretacic---Prather. 173 25 feet in thickness and extends from Bay View avenue in the direction of Hiltons some 800 feet. It is a sand as shown when separated and examined under the miscoscope although it appears at first sight to be a compact clay. It is sometimes found as one bed, or may be made up of a num- ber of small beds or lenses of only local extent varying in thickness from 2 feet to 8 feet (see lenses 4 and 5). The color varies from white to yellow, salmon, brown, orange, and red. It is made up almost entirely of quartz grains with grains of iron, probably magnetite, mica, and some glauconite. The quartz grains are both angular and round- ed and are generally of uniform size, although larger and more rounded quartz grains are noted. It rests above the Marshalltown clay and below the Navesink and Mt. Laurel, although the upper Marshalltown clay seems to be about the same age. Sometimes it is coarse like an ordinary sand, and again it is finer grained like a clay. This is probably the upper part of the Hazlet sand of Clark. Part of it may correspond to the Wenonah sand of the New Jersey survey, although on account of local variation it does not seem to’ fit this so well, and is therefore given a local name. Bay View Avenue Lenses, (1), (3), (4), and (5). These four lenses are included as part of the Bay View Avenue sand and as part of the Mt. Laurel sand. No. (1) is 4 feet thick and 120 feet long; No. (3) is 4 feet, 5 inches thick and 120 feet long; No. (4) is 2 feet thick and 130 feet long; and No. (5) is 2 feet thick and 70 feet long. No. (1) is very fine grained and of a light color. It contains quartz and mica but has so much fine clay as to render it a clay rather than a sand, and causes it to break into hard lumps. No. (3) is much coarser and more arenaceous than No. (1) and contains more glauconite and more quartz and less - fine clay. It is a brown color and readily separates into a sand. Nos. (1) and (3) are part of the Mt. Laurel sand. No. (4) is fine grained like No. (1) but of coarser grain. It breaks up into lumps and has so much fine clay as to make it a clay rather than a sand. It contains quartz and mica but the clay predominates. It is of a light grey color and contains very little glauconite. 174 The American Geologist. SepveD per No. (5) is a brown sand but fine grained and contain- ing much fine clay. The grains of quartz and mica are also very small. Nos. (4) and (5) are part of the Bay View Avenue sand. Marshalltown Clay. The bed here identified is from 15 feet to 43 feet thick and extends from 200 feet from Bay View avenue to near Hiltons station. It represents part of the Hazlet sand of Clark and would correspond to the (Clay marl 4) Marshall- town bed of Knapp. It is a dark colored clay which varies in color from black to a light grey, when it has a silvery or micaceous appearance. Examined under the microscope it is found to be composed largely of clay and quartz grains, and some mica flakes. It is finer grained, darker in color and very different from the beds, one above, and the other below it, for they are arenaceous (silic arenites) and composed largely of quartz grains, while this bed is more of a clay or clay marl. It might be suitable for making brick or certain grades of earthenware. It is finer grained than the Navesink which rests above it in part of the sec- tion, ‘but, im the rest, of the section, the bed calledmiiaw View Ave)nue sand comes in between. It contains very little glauconite and is generally very fine grained and con- tains much fine quartz and mica and a good deal of fine clay. Columbus Sand. This generally occurs at the base of the sections from Bay View avenue to near Hiltons. It represents the Upper Hazlet sand of Clark. It seems to be a part of the over- lying bed in certain instances and lenses (6) and (7) of this sand are included in the Marshalltown clay above. It varies in color from white to yellow and red, may even assume a slate color owing to the clay present in it. It contains interstratified layers of slate colored clay which is very smooth and fine grained. It is made up largely of quartz grains of variable size, and often highly colored. It contains numerous flakes of mica and many grains of glauconite scattered through it, some of which have been altered to iron compounds. Besides the color, the pieces of clay and the mica flakes are most characteristic. It varies in thickness from 5 feet to 25 feet although on ac- ‘enuesAW MOIA AVG WMOIg AIW Syne’, vse1yg, WOES eS eS ae as ee a ee = 4 4 79 ij bile AZ AA & v2 I 37zvH GM WS JAM BAY M3IA “LBA °° LAr 638 Why K SS vod] / ZY WS LI — a = i AIP SRR seeeate LUV) ~~ — anus snawn79 \\ SRV7D WMAOLTTVHSUYW ONWS BAWSAV MIA EOE ION YS TINVILW SN31YNISINYN Y yuisanwn ZY 7 sar SONVIHIH WINWTLY 4” MOILOTS ANVE G34 HINVYE WOT wv/ewnroa Reores ON 3947 ‘xX ALVId ‘IAXXX “I0A ‘LSINOTOAY NVOIUANY AHI, Atlantic Highlands Cretacic---Prather. 175 count of being at the base, it is not always completely ex- posed. SECTIONS. The following sections taken at intervals give the de- tail of the formations: Section 250 feet from Bay View Avenue. Conglomerate at top..... 2ft. Columbian gravel Samples Shay aVi ll Se Gees, Volceinne Cenenen 3ft. Long Branch. Bl & B2 Light greensand ........ 10 ft. Bowes: a Dark greensand ......... 6 fils : a Fossil bed with glauconite Navesink. STAINS ras «s,s peateiMans A aves aos o 6 ft B5.....- Light clay (cream colored) with few glauconite +} Mt. Laurel sand. grains (Lens 1)..-..... 4 ft. : B6 & Ba prown clay containing } much quartz grains and | Bay View Avenue mica and with glauco- nite grains disseminated a vp DPer eieoueh! Wt ©. fo. eers 2 cs 12 ft a AT Biseas se Dark clay made up largely 7} . (Hazlet of clay and a good many | Marshalltown sand) quartz and mica grains 11 ft. j Light gray sand largely ) quartz with some mica | Columbus with interstratified lay- j Sand. ENS OMUClAY: fants 2 tte crs 6 ft. | Section 450 feet from Bay View Avenue. Quartz pebbles (conglomerate) at top Columbian Samples. DOC Te ee creda thie we cieie ale Miereieslelts, a anevels. 6 QuarizeSand iio ue eee sak sss 5 feet Long Branch C1 Light greensand chiefly glauconite..... "ft. ] Grains cemented. | d Cb Dark greensand most all glauconite....5 ft. ; Navesink Grains cemented together (Lens 2). 176 The American Geologist. Sepremveraaae C2 Brown clay, light brown ] i color and with much Mt. Laurel Quartz (ens Galerie. 4.5 ft. | C3 Brown clay, still lighter ih color than preceding but composed of same ma- terials (Lens 4)........ Dots C4 Brownish yellow clay made | ! fn View Avenue | i} | Upper up largely of quartz Mata ecaing (mens 5) eeeeee ite sand. pet pe: C5 Light brown clay with : quartz grains and flakes sand) of mica embedded in the clay ground mass.. 15 ft. | } ) C6 Dark grey clay with fine 1 QuanrtzaSrains! eee 12 £t Marshalltown C7 Light grey sand largely quartz and some mica with interstratified lay- CLSMODmC] aya wets mee are 8 ft. | : | ‘Columbus sand. Section in bend of Creek 800 feet trom Bay View Avenue. Columbian 3ft. Samples. Quartz pebbles and sand........ 20 ft. « Long Branch 5 ft. Redbank 12 ft. D2 Greensand dark colored and made up largely of glau- conite grains cemented and with some grains of quartz and mica scatter- Cd tthrougn (A) sos cro iene 10 ft Navesink of clay and a good many Marshalltown D1 Dark clay made up largely quartz and mica grains. 35 ft. | Upper Matawan, or Dark gray sand, largely J quartz with some mica and interstratified with LaVersvOn(Claviveasieiaeeiner Cnet. i ) r (Hazlet sand) Columbus sand | * Both the Bay View Avenue sand and the Mt. Laurel sand grade into the Marshalltown clays here and disappear. EK2 E3 r4 E5 ES Atlantic Highlands Cretacic---Prather. 177 Section 1250 feet from Bay View Avenue. 5 ft. 5 ft. ’ Quartz pebbles at top....... Quartz sand eecvreceesceceeeecen Quartz sand, salmon color- ed made up of quartz and some mica and magne. tite grains 6 ft. Light colored clay with quartz and mica in large flakes and some glau- conite but glauconite ratner rare I | 5 } | Dark greeu and layers com- posed of glauconite erains cemented Light greens and layers.... HORE ) See | Dark grey clay made up largely of clay with much ! quartz and mica 25 ft. \ Light and dark grey to yel- low sand with interstrati- fied layers of clay. The material is largely grains of quartz with large mica flakes and some grains cf slauconite Ome CO OO are - Marshalltown Columbus sand Columbian gravel Long Branch Redbank Navesink Navesink Upper Matawan or (Hazlet sand) ) | Section 1600 teet from Bay View Avenue. 10 ft. Columbian 5 ft. Long Branch ee ee Samples. Sond ceneeeceecces ceoeetanseoacese Red sand changing from dark red to yellow salmon, grey, &¢., largely quartz 9.5 ft. Redbank light greem sand. --..-...-0-+-- Dark greens and nearly all glau- conite grains cemented _ to- SZ OUMERN rvstteie chevel tas ieueliejaisiciels\slo <1 =)x ters Navesink —— $$ >= 5 ———_ _ @),6) pp e\,0) "ee: (etre).0 (0 ae Dark green clay made up of | quartz and mica grains in clay 25 ft. Marshalltown | Matawan > (Hazlet | Columbus sand | Sand) J Light colored quartz sand with layers of inte: stratified clay.. l 5 fh.) Gl, where they were taken. 178 The American Geologist. Repteier ae Section 3960 feet from Bay View Avenue. meni dorsags AU) e) Ps Columbian SAN’ <2 coe eee etaiorels er sieererae dete eee yd Long Branch Red sand largely made up of quartz } grains with some hard cemented > Redbank WHOA sopoocde. Sosrodocoondadoconauds 90 ft ) G2, G3 Glauconite beds with much | clay and quartz grains near the top and with less quartz and more glauconite near the mid- > Navesink dle and bottom, and with numerous fossils es- | pecially in bed 3 or basal i MOLtLONTOn Dede. eee 20 ft. | These sections and the intervening parts are shown on the drawing made to scale from measurements and notes taken in the field (Plate x). to scale on tracing cloth and taken into the field and the beds separately traced out and mapped and the intervals filled in while in the field: The letters Art; Bi; &c; refer to samples of the beds, located on the section at the points The sections were drawn (See also plates viii and ix). Mineralogical Contributions—Hobbs. 179 CONTRIBUTIONS FROM THE MINERALOGICAL LABORATORY OF THE UNIVERSITY OF WISCONSIN. By WILLIAM HERBERT Hosss, Madison, Wis., Assisted by others. PLATE XI. In the following pages have been brought together a number of brief statements which it is thought are deserv- ing of being placed upon record. Undertaken from time to time as material has come tc ihe laboratory they have been allowed to wait until collectively they had a value which individually would not belong to them. The econ- omical and mineralogical work has been carried out in part by the professor in charge of the department, or by his students, but generally in collaboration. Credit for work is given in connection with the individual contributions. a, Analysis of Huebnerite from Dragoon Summit, Ariz.* by S. V. Peppel. The specimens of this mineral are cleavage blades from large hair brown crystals two inches or more in length. An analysis of them yielded the fol- lowing results: Se ond ieee ee MAREE: 1.10 ROC eee a OO hes ne 75.10 ROM ee en en tee FP 22.87 FSO) ells Se AER NR 6” ein ail es Re a 81 * 99.88 The re-calculated analysis-excludes the silica, which is probably included material. This analysis appears below in column 1, and in column II is given the theoretical com- position of pure huebnerite. WOE eter ee bbe lelscaned Ve wean %6 76.13 76.6 TVET etcatenct steno meene bles okenet oe 23.15 23.4 INNO) gis'8 Win ing gon Goamoor 82 100.00 100.00 b. Quartz Crystals from near Las Vegas, N. M. These specimens were received from Mrs. A. P. Buck, East Las Vegas, N. M. They constitute numerous double-termin- ated crystals of clear colorless quartz of great pellucidity resembling in habit the Herkimer quartzes from New York * This occurrance has been described by W. P. Blake in the Mineral Industry, vol. 7, 1899, pp. 720-722. + And oxides of columbium group, if present. 180 The American Geologist. _. September, 1905 state. In common with Herkimer quartzes, also, these crystals are found with much lustrous black material which glows and becomes white on ignition and appears to be in part like the included material of the Herkimer crystals. The crystals sent are somewhat smaller than the average of those obtained from Herkimer county, but they yet re- semble them quite closely. These crystals are re- ported by Mrs. Buck to occur in “‘veins” in the high country near Las Vegas, hundreds being there found in each shovel- ful of earth, and the best crystals being obtained in pockets along with the lustrous black material of which, however, only a small amount was included with the sample. ¢. Calcite, Sphalerite, and Pyrite from Oshkosh, Wes- consin. The specimens of these minerals were collected from the dolomyte quarry one mile southwest of the city of. Oshkosh and presented to the university of Wisconsin by Mr. T. J. Thorson. The calcite shows two habits; one hav- ing the form r, (1011) unmodified, the other exhibiting the forms f, —2R (0221); v, R® (2131) ; e, —AR, (or12); m, OP (1010) - andr, R (1011), the latter form small. The sphalerite shows the ordinary combination of do- decahedron and trapezohedron (311). ad. Minerals from Eau Claire, Wrseonsin. Specimens of pyrite, marcasite, sphalerite, chalcopyrite, and dolomite have been obtained from this locality. The pyrite occurs in well formed octahedral crystals up to 1% centimeter in diameter, with the cube and dodecahedron truncating the angles and edges respectively. The crystals show a green- ish to bluish iridescence. Marcasite occurs together with the pyrite and in the common tabular forms which are bounded by the base, unit prism, and one or more of the brachy-domes y. and 1. The dolomite occurs in a simple rhombchedron, while the chalcopyrite is found only massive. e. Dolomite and white Zinc Oxide from Highland, Wisconsin. he dolomite occurs in lenses of small gray and curving faced rhombohedrons with dimensions of a few millimeters only. The specimen of zinc oxide was pre- sented by Mr. Richard Kennedy, mining expert, resident at Highland. This material is quite massive and forms a coat- Mineralogical Contributions—Hobbs. 181 ing on the limestone of the district. Its surface is botry- oidal and the mineral has the appearance of having been sublimed upon the surface. In color it is almost pure white resembling magnesite; but ignited on charcoal it becomes yellow, cooling to white, and with cobalt solution gives the usual color of zinc compounds. It dissolves readily in hy- drochloric acid. i jf. Other Unreported Occurrences of Wisconsin Mtn- erals, Other minerals which are not upon record, and which have been found in Wisconsin are given below. Pyrrhotite from Mountain post office, where it is found in quite extensive deposits entirely massive in appearance. Barite from Belmont, which occurs with brown blades as imperfect crystals up to 4 or 5 centimeters in length. Limonite pseudomorphs after marcasite from Madison. These latter pseudomorphs show the combination of the prism m with either v or 1. Malachite; Baraboo, Sauk county. Chalcopyrite, cuprite, and malachite; Boscobel. | Chalcopyrite, malachite; Soldier’s Grove and Wayne. Graphite; Marshfield. g. Minerals from Helderberg Limestone of Tiffin, Ohio. The University of Wisconsin is indebted to professor M. E. Kleckner of Heidelberg university located at Tiffin, for a small collection of minerals from the quarries at that place. According to professor Kleckner the limestone of the dis- trict is part Niagara and part Helderberg, and it is in the latter that the crystallized minerals have been found. They occur as the lining of cavities some of which have a diameter, as indicated by specimens received, of one to two decimeters. Certain layers in one of the quarries have many filled cavities of cylindrical shape which have become known to the quarry-men as “plugs.” These seldom ex- tend through more than a single layer of the limestone. The minerals of this plug are the same as those filling the other cavities; namely, calcite, celestite, fluorite, and sphal- erite. The calcite is the most abundant of the minerals lining the geodes, and occurs in two different habits. The first 182 The American Geologist. cag cee noah 2)” shows small yellow crystals % centimeter in length with the habit determined by the form f, —2R (0221) unmodified. The other type shows larger crystals of “dog tooth” habit which are often several centimeters in length. These crystals like the others are of a pale yellow color and their habit is determined by d, —8R (0881) with which is gen- erally present e, —'%4R (o112) and t, %4R* (2134) and some- times v, R® (2131). The faces are more or less dull, and frequently vicinal, but allow their angles to be read with sufficient accuracy for a determination of the forms. The celestite occurs in tabular to bladed crystals vary- ing in size from one-half to several centimeters in their di- mensions. The color is a pale blue, as in the case of the well known celestite from Put-in-Bay on lake Erie. The base is always the tabular plane and the macro-diagonal the axis of greatest development. The forms present are, in the order of relative size, c, OP (oor); d, %P (112); 0, Po (Ort); 1m, CORA 10) eiind'z).P)(i11). The crystals of fluor spar are associated with the cole and the celestite in the cavities. They are cubes and cubo- octahedrons made up of well-rounded sub-individuals, and sometimes attain to a size of two or more centimeters along . the cubic edge. Some crystals are nearly colorless and quite clear; others have areas colored yellow, but the ma- jority of those examined have a rich brown color between that of smoky quartz and of the well-known brown siderites from Roxbury, Connecticut. A mineral much less common in the geodes is sphaler- ite, which appears in distinct crystals a centimeter or more in diameter. The color is that of a light “rosin jack” and would match the color of the well known sphalerites from Joplin, Missouri. Like the latter, also, the combination found upon the Tiffin sphalerite is that of the dodecahedron with the common trapezohedron (311). h. Calctte from Grand Rapids, Michigan. Specimens of calcite from Grand Rapids, Michigan were received from Mr. J. C. Ulman of Ashland, Wisconsin. He collected them in 1894. According to his statement the crystals are found in seams and cavities in the limestone which forms the bed Mineralogical Contributions—Hobbs. 183 of the Grand river, coffer dams having been built and the rock quarried both for lime and for road metal. The lime- stone is traversed by a vertical vein of barite, containing well developed crystals. Two miles down the river the limestone dips under the well known gypsum beds of the vicinity. The rock in which the crystals here described were found, is a dark gray to white compact limestone with cavities which in many of the specimens were lined with a film of pyrite, to which the calcite crystals are attached. These crystals have been studied at the university by Mr. W. M. Kennedy. The habit of the calcite is either scalen- ohedral or rhombohedral, the latter variety being white and the former when found alone of a brownish-yellow color. Twins are common, the twinning plane being a face of the fundamental rhombohedron. Superimposed upon some of the larger crystals are numerous smaller and much distorted individuals so flattened as to resemblein form the tooth of a shark, the orientation being, however, the same for both larger and smaller crystals. The following forms were observed: ; r, R (1011) View 208 (7. a3) ¢, —5& R (0554) Db, Rz (11. 16. 5 6) X,—2R (0994) and d, —3 R (0331) I, —2 R (il. 0.11. 3) doubttat Mele tt (On 11), 12-8) ; vy, R® (2131) 184 The American Geologist. Reptemibe sere Fig. 1. Development of calcite crystals from Grand Rapids, Michigan. The angles which determined the forms were as follows: Obs. Cale. Diff. dd’ (polar) 84°23’ 84°32’ — 9,’ py’ 35°33" 35°36’ —3’ TV 29° 1b’ 29cr 28 +3’ tb tb’ 32°40’ 32°36’ +4’ MM’ AQ 4 40° 3’ 0 r M ase UN 32°57" +3’ rw 29°52’ 29°54’ —2’ ip fh AGC 0” MoS e +3’ rl 106° 0’ 105°59’ +1’ The new form R& was found on a number of crystals and was accordingly determined. The form | was found on but one crystal, though here with a large development. See ties: The crystals represent a number of distinct habits among which is the barrel-shaped type of fig. 2. There is also another “nail-head” type, and a very steep rhombohe- dral type. Fig. 2. Barrel-shaped type of calcite from Tiffin, Ohio. t. Epsomite and Alunogen from. the Cripple Creek District, Colorado. These specimens which were among the collections of the university of Wisconsin have been analyzed, the first mentioned by Mr. W. O. Hotchkiss, arid the last mentioned by both Mr. Hotchkiss and Mr. R. M. Chapman. Their results follow: ‘*Epsomite’”’ from Cripple Creek District, Colorado. Analyzed by W. O. Hotchkiss. Wik OSS er ainc ao oaas oa oem cada cdoKsdo0 6.0 0 Oa 6 19.35 SOROS etaoe odo igbomiagas qecaoucscobdsoGcGe fe 38.51 1EELO) GoGo S eerts sane Mrishobiash.s Lepoeens eanatfcee Tame yererononornenelens 42.03 ~y | \ '’ &. ie zs A e wl ‘4s . i on neon AMERICAN GEOLOGIST, VoL. XXXVI, PLATE XI, METALLIC COPPER, SOUDAN, MINN Mineralogical Contributions—Hobbs. 185 “‘Alunogen” from Cripple Creek District, Colorado. Analyzed by W. O. Hotchkiss and R. M. Chapman. Hotchkiss. Chapman. INH OF So encom Cee Nemoe Mena o csr 8.28 9.41 INGEHONs oS 5dSoabe 6 ana Ute ono 14.44 4.40 BOs et aiehaie sails) ohstarmisyaveve's, siete FANS OAS 43.74 IED Gewese code toogogntog aor 43.86 43.86 100.64 101.41 The close similarity of the two minerals makes it diff- cult to obtain a perfect separation of them, and this chiefly explains the variation observed between the analysis quoted. Jj. Crystallized Copper from Soudan, Minn, A very interesting and almost unique example of metallic copper in association with hematite is the occurrence at the Minnesota mine in the Vermilion iron-bearing district of Minnesota. As this occurrence does not appear to have been figured, the beauty of the films and trees seems to warrant its repre- sentation, which is given in plate x1. Although the occur- rence has been described,* it does not appear to be well known, the place of publication not being well known to mineralogists. The occurrence is also casually mentioned by Clements.i Together with the hematite in association with the copper are found cuprite, malachite, and azurite. The copper minerals occur, in a narrow seam in brecciated hematite, the only place where it is found in the region or in any of the iron-bearing districts of lake Superior. This rare occurrence should be considered in connection with the discovery by. Haworth of thin films of native copper in red clay shales near Enid, Oklahoma.? In both occurrences the copper is extremely limited and generally found in thin films upon apparent fissures. Though the Soudan occur- rence was apparently not known to Haworth at the time his paper was read, he. has suggested the same explanation, namely ; the reduction of the copper by the oxidation of the ferrous iron compound. *J. H. Expy, and CHARLES P. BERKEY. Copper minerals in hematite ore. The Year Book of the Society of Engineers, university of Minne- sota, 1897, pp. 108-117. Reprinted from the Proceedings of the Lake Su- perior Mining Institute, vol. 4, 1896, pp. 69-79. + J. Morgan CuiemeNtTS. The Vermilion Iron bearing district of Minne- sota. Mon. 4, U. S. G. S. 1908, pv. 112, 184. N. H. WincHeti Metallic Copper. Final report, Minnesota Geological Survey, vol. 5, p. 885, 1900. 186 The American Geologist. a aag It is interesting to note that beautifully crystallized copper has been produced in trees resembling the aborescent native copper of the Soudan occurrence through electroly- sis.* This copper was formed at the lower corner of a full sized kathode operating under bad conditions in an insoluble anode tank, presumably with very high current density. REVIEW OF RECENT GEOLOGICAL LITERATURE, Structure of some Cephalopods, by R. RurpEmann.- [Report of New York State Paleontologist 1903, Albany, 1905]. Notes on the apical end of the siphuncle in some Canadian Endo- ceratidae, &c. by J. F. WuitrEeaves [American Geologist, Jan. 1905). Ueber die eocambrische Cephalopodengattung Volborthella, SCHMIDT, von A. Karpinsky, (Verhandl. russ: miner. Gesell. Bd. xli, li, pp. 31-42]. These papers with that of G. Holm 1895 on the formation of the endosiphon in the Endoceratide help greatly to a proper under- standing of the initial stage of the shell in the early cephalopods. Esvecially is this the case with the first-named essay, based upon excellent material from the oldest Ordovician limestones of lake Champlain. The essay is valuable not only for what it tells us about the Beekmantown cephalopods, but also for the synopsis which it contains of the work of other observers in this field of re- search—Barrande, Dewitz, Whitfield, Dawson, Hyatt, Holm, Foord, Clarke and others. Ruedemann’s work is based chiefly on the species Camerocera, brainerdi Whitfield, and fully describes the delicate chitinous and chitino-caleareous parts of the envelope in this species, which pre- ceded the formation of the calcareous shell. The assumption of the calcareous habit is plainly shown in the individual history of these shells, as it is in several of the Hyolilhide of an earlier date. Dr. Ruedemann’s work is abundantly illustrated with wood cuts in the text and a series of plates at its close. C. brainerdi began in a small cylindrical tube (endosiphotube, page 320) which became dif- ferentiated by the addition of an outward enclosing tube (endosi- phocoleon). The first named tube fades out or loses its chiten, + E. HawortH Native copper near Enid, Oklahoma, Buli.’ Geol. Soc. Am., vol. 12, 1901, pp. 2-4. f *LAWRENCE ADDICKS. Electrolytic copper, Electro-chemical and metallurgical industries, vol. 3, 1905, p. 167, fig. Review of Recent Geological Literature. 187 leaving the latter as the endosiphon, Chitenous or sub-chitenous supports (endosiphoblades, &c.) passing to the walls of the siphun- cle held this endosiphon in its place. Gerard Holm has found quite similar structures, though not so complete, in Vaginoceras basaliforme. The stage of the single ° worm-like tube in Cameroceras is rightly regarded by Ruedemann as an important accession to our knowledge of the initial structures in the early cephalopods. Dr. Whiteaves’ paper also has plates, two in number ,which present the characters of two new species of Endoceratites, based on the siphuncle, from Canadian localities, Nanna primaevus and N. kingstonensis. In the latter which is represented by casts of the siphuncle, the impression of the septal necks is finely shown, and the forward curve of the septal rings is well marked. A. Karpinsky has made a fresh study of Schmidt’s genus Vol- borthella (V. tennuis) from the “blue clay” of the Lower Cambrian of Reval in the Baltic provinces of Russia. He sustains the view of Schmidt that this organism is a cephalopod, since he found it characterized by a siphonal tube. It is a long space in geological time between this organism and the oldest known chambered ceph- alopod; perhaps the connection between Volborthella and the lat- ter has been through some of the shells classed with the Hyolithide to which Volborthella bears a close resemblance. Between the “blue clay” and the Beekmantown horizon four Cambrian faunas intervene—Paradoxides, Olenus, Peltura and Dictyonema—in which no recognized orthoceratites are known. Ww. U, The Copper Handbook, a Manual of the Copper Industry of the World. Vol V, for the year 1904. Compiled and published by Horace J. STEVENS. Pages 882. Houghton, Mich., 1905. This is the fifth yearly issue of a very comprehensive and use- ful handbook. It contains chapters on the history, geology, chem- istry and mineralogy, metallurgy, and uses of copper; a glossary of mining terms; details of copper deposits in all parts of the world; a very extensive alphabetic list, in 683 pages, describing all the copper mines of the world, and noting all companies engaged in copper production; and statistics, in 38 pages. Concerning the very important and recent uses of this metal for telegraph and tele- phone wires and a multitude of other electric appliances, the com- piler writes: “Copper is the foundation of the Electric Age, just as it was the fundamental metal in the Age of Bronze, some millenniums ago. * * * A full enumeration of the electrical uses of copper would require a volume.” WU. The Honorable Peter Whit». A Biographical Sketch of the Lake Superior Iron Country. By Ratreu D, WILLiams Pages 205; with many portraits and other illustrations. Cleveland, Ohio, 1905. A very interesting biography of the most prominent promoter of the mining of iron ores in the upper peninsular of Michigan is 188 The American Geologist. 8 decors) 2 here presented, with chapters also on the great iron ranges of Wisconsin and Minnesota. The marvelously large and growing traffic that passes through the Sault Ste. Marie canals, both on the United States and Canadian sides, and the semi-centennial celebra- tion of the opening of the first canal there, are very fully treated. Not only biography and history, but the economic development of the lake Superior region, so far as it has depended on iron ore production, are vividly depicted; and in all the wonderful progress of that region during the past fifty years the subject of this bio- graphy was a conspicuous part. WwW. U. MONTHLY AUTHOR’S CATALOGUE OF AMERICAN GEOLOGICAL LITERATURE ARRANGED ALPHABETICALLY. ALDEN, WM. C. The Delavan Lobe of the Lake Michigan Glacier of the Wis- consin stage of Glaciation and Associated Phenomena. (U.S. G. S. Prof. Pap. No. 34, pp. 101, Pls. 15, 1904.) ANDERSON, NETTA C. A Preliminary List of Fossil Mastodon and Mammoth Remains in Illinois and Iowa. (Augustana Lib. Pub. No. 5, pp. 9-48, 1905). ARNOLD, RALPH. Coal in Clallam County. (U.S. G. S. Bull. No. 260, pp. 413-422, 1905). ASHLEY, GEO. H. Coal in the Nicholas Quadrangle. (U. S. G. S. Bull. No. 260, pp. 422-429, 1905). BAGG, R. M., Jr. The Minerals of Maguarichic. (Eng. Min. Jour. vol. 80, p. 2, July 6, 1905). BAIN, H. FOSTER. Soft-Lead Resources of the United States. (Mining Mag. vol. 12.p2 19) July, L905). * BAIN, H. FOSTER. Principal American Fluorspar Deposits. (Min. Mag., vol. 12, No. 2, pp. 115-119, Aug., 1905). : BASCOM, F. Piedmont District of Pennsylvania. (Bull. Geol. Soc. Am., vol. 16, pp. 289-328, Pls. 48-64, 1905). Monthly Author’s Catalogue. 189 BEEDE, J. W. (and E. H. SELLARDS). Stratigraphy of the Eastern Outcrop of the Kansas Permian. (Am. Geol., vol. 36, pp. 83-112, Aug., 1905). BURCHARD, E. F. The iron ores of the Brookwood Quadrangle, Alabama. (U. S. G. S. Bull. No. 260, pp. 321-335, 1905). BUTTS, CHARLES. Warrior coal basin in the Brookwood quadrangle, Alabama. (U- S. G. S. Bull. No. 260, pp. 357-382, 1905). CLARKE, F. W. A pseudo-serpentine from Stevens County, Wash. (U.S. G. 8. Bull. No. 262, pp. 60-72, 1905). CLARKE, F. W. (and GEO. STEIGER). On “Californite” (U. S. G. S. Bull. No. 262, pp. 72-75, 1905). CROSBY, W. O. Genetic and Structural Relations of the Igneous Rocks of the Lower Neponset Valley, Massachusetts. [II.] (Am. Geol., vol. 36, pp. 69-83, Aug., 1905). DALE, T. NELSON. Slate investigations during 1904. (U.S. G. S. Bull. No. 260, pp. 486-489, 1905). DARTON, N. H. Coal of the Black Hills. (U.S. G. S. Bull. No. 260, pp. 429-434,. 1905). DARTON, N. H. Zuni Salt Deposits in New Mexico. (U.S. G. S. Bull. No. 260, pp. 566-567, 1905). DARTON, N. H. Discovery of the Comanche Formation in Southeastern Colorado. (Science, vol. 22, p. 120, July 28, 1905). DIEEER, J: Ss: So-called iron ore near Portland. (U. S. G. S. Bull. No. 260, pp. 343-348, 1905). DILLER, J. S. Coal in Washington near Portland, Ore. (U.S. G. S. Bull. No. 260, pp. 411-413, 1905). EASTMAN, C. R. A Brief General Account of Fossil Fishes. (Geol. Sur. N. J. Ann. Rep. for 1904, pp. 27-67). ‘ EASTMAN, C. R. The Triassic Fishes of New Jersey. (Geol. Sur. N. J. Ann. Rep. for 1904, pp. 67-131, pls. 14). 190 The American Geologist. september eee ECKE iE wc. Limonite deposits of eastern New York and western New England. (U. S. G. S. Bull. No. 250, pp. 335-343, 1905). ECKEE, Enc; Tron ores of northeastern Texas. (U.S. G. S. Bull. No. 260, pp. 348-355, 1905). ECKEE, E..C: Portland Cement resources of New York. (U. S. G. S. Bull. No. 260, pp. 522-531, 1905). iECKEL, E. C. Pyrite Deposits of the western Adirondacks. (U.S. G. S. Bull. No. 260, pp. 587-589, 1905).’ FULLER, MYRON L. Geology of Fishers Island, New York. (Bull. Geol. Soc. Am., vol. 16, pp. 367-390, pl. 66, 1905). GILBERT, G. K. Systematic Asymmetry of Crest-Lines in the High Sierra of Cali- fornia. (Bull. Sierra Club, vol. 5, No. 4, pp. 279-287, pls. 4, June, 1905). j ‘GRISWOLD, W. T. Pittsburg coal in the Burgettstown quadrangle. (U. S. G. S. Bull. No. 260, pp. 402-411, 1905). ’ ‘HALL, M. R. (and J. C. HOYT). Progress of Stream Measurements. (U. S. G. S. Wat. Sup. & Irr. Pap. ‘No. 127, Part 4, pp. 192, 1905). HAMILTON, S. H. (See KUMMEL, H. B.) HARRIS, G. D. Bulletin of the Louisiana Geological Survey No. 2, pp. 49, Pls. 11-16, 1905). a HILL, ROBT. T. Source of volcanic water. (Eng. Min. Jour., vol. 80, p. 13, July 6, 1905). HILLEBRAND, W. F. (and F. L. RANSOME). On Carnotite and Associated Vanadiferous Minerals in western Colorado. (U.S. G. 8. Contributions to Mineralogy, Bull. No. 262, pp. 9-32, 1905). HILLEBRAND, W. F. (and S. L. PENFIELD). Some Additions to the alunite-jarosite Group of Minerals. (U. S. G. S. Bull. No. 262, pp. 32-42, 1905). HILLEBRAND, W. F. (see LINDGREN, WALDEMAR). HILLEBRAND, W. F. Two Tellurian Minerals from Colorado. (U.S. G. S. Bull. No. 262, pp. 55-58, 1905). HILLEBRAND, W. F. (see SCHALLER, W. T.) Mouthly Author's Catalogue. IQE HILLEBRAND, W. F. _ The composition of yttrialite, with a criticism of the formula assigned to thalénite. (U.S. G. S. Bull. No. 262, pls. 61-69.) HOYT, J. C. (see HALL, M. R. and TAYLOR, F, N.) JOHNSON, W. D. The Grade Profile in Alpine Glacial Erosion. (Bull. Sierra Club, vol. 5, No. 4, p. 271, pls. 4, June, 1905). JOHNSON, R. D. O. Tennessee Phosphate. (Eng. Min. Jour., vol. 80, p. 204, Aug. 5, 1905). KEYES, C. R. Zine Carbonite Ores of the Magéalena Mountains. (Min. Mag. vol. 12, No. 2, pp. 109-114, Aug., 1905). KEYES, C. R. Bisection of Mountain Blocks in the Great Basin Region (Ab- stract). (Iowa Acad. Sci.) KEYES, C. R. Geological Structure of the Jornado del Muerto and adjoining Bolson Plains. (lowa Acad. Sci.) KEYES, C. R. Northward Extension of the Lake Valley Limestone. (lowa Academy of Sciences). KEYES, C. R. The Fundamental Complex beyond the Southern End of the Rocky Mountains. (Am. Geol., vol. 36, p. 112, Aug., 1905). KEYES, C. R. Ore deposits of the Sierra de Los Caballos. (Eng. Min. Jour., vol. 80, p. 149, July 29, 1905). KUMMEL, H. B. (and S. H. HAMILTON). A Report upon some molding Sands of New Jersey.) Geol. Sur. N. J., Ann. Rep. 1904, pp. 187-244). KUMMEL, H. B. The Mining Industry. ((Geol. Sur. N. J., Ann. Rep. 1904, pp- 291-303). LAKES, A. Igneous rocks in ore deposition. (Eng. Min. Jour., vol. 80, p. 196, Aug. 5, 1905). LINDGREN, WALDEMAR. Minerals from the Clifton-Morenci District, Arizona. (U. S. G. S., Bull. No. 262, pp. 42-55, 1905). LULL, PROF. R. S. Restoration of the Titanothere Megacerops. (Am. Nat., vol. 39, p. 419, July, 1905). 192 The American Geologist. Septemper neue MATTHEW, W. D. Notes on the Osteology of Sinopa, a primitive member of the Hyenodontide. (Proc. Am. Phil. Soc., vol. 49, p. 69, Apr., 1905). \ MATHEWS, EDW. B. Correlation of Maryland and Pennsylvania Piedmont Forma- tions. (Bull. Geol. Soc. Am., vol. 16, pp. 329-346, 1905). MATHEWS, EDW. B. (and W. J. MILLER). Cockeysville Marble. (Bull. Geol. Soc. Am., vol. 16, pp. 347-366, IPI 65; 1905) MILLER, W. J. (see MATHEWS, EDW. B.) MOFFIT, FRED H. The Fairhaven Gold Placers, Seward Peninsula, Alaska. (U.S. G. S., Bull No. 247, pp. 81, Pls. 14, 1905). NEWLAND, DAVID H. The Mining and Quarry Industry of New York State. (Bull. 347, N. Y. Ed: Dept: pp: 909-979, 1905). PAINTER, R. H. 4 Pyrite mining in Virginia. (Eng. Min. Jour., vol. 80, p. 148, July 29, 1905). PECK, F. B. The Tale Deposits of Phillipsburg, N. J. and Easton, Pa. (Geol. Sur. N. J. Ann. Rep. 1904, pp. 161-185). PEET, CHAS. EMERSON. Glacial and Post-Glacial History of the Hudson and Champlain Valleys. (Separate from Jour. Geol., vol. 12, July and Oct., 1904). PETERSON, O. A. Preliminary Note on a gigantic Mammal from the Loup Fork beds of Nebraska. (Science, vol. 22, No. 555, p. 211, Aug. 13, 1905). PURINGTON, C. W. Gravel and Placer Mining in Alaska. (U.S.:G. S., Bull. No. 263, pp. 225, pls. 42,.1905). RANSOME, F. L. The Cceur d’ Alene District. (Mining Mag., vol. 12, p. 26, July, 1905). SAMPLE, C. C. Amber in Santo Domingo. (Eng. Min. Jour., vol. 80, p. 259, Aug. 12, 1905). SCHALLER. W. T. (and W. F. HILLEBRAND). Notes on lawsonite. (U.S. G. S. Bull. No. 262, pp. 58-61, 1905). SCHALLER, W. T. Dumortierite and Mineralogical Notes. (U. S. G. S. Bull. No. 262, pp. 91-121, 1905). Monthly Author's Catalogue. 193 SHALER, M. K. (see TAFF, J. A.) SELLARDS, E. H. (see BEEDE, J. W.) SINCLAIR, WM. J. New or Imperfectly known Rodents and Undulates from the John Day Series. (Bull. Dept. Geol. Univ. Calif., vol. 4, No. 6, pp, 125-143, Pls. 14-18, 1905). : SINCLAIR, WM. J. The Marsupial Fauna of the Santa Cruz Beds. (Proc. Am. Phil. Socsnvol. 495 ps io, Apr, 1905). SMITH, W. S. TANGIER. (See ULRICH, E. O.) SMITH, G. O. The granite industry of the Penobscot Bay quadrangle. (U. 8. G. S. Bull. No. 260, pp. 489-493, 1905). SPENCER, ARTHUR C. Progress of Work in the Pre-Cambrian Rocks. (Geol. Sur. N. J., Ann. Rep. 1904, pp. 247-253). STANTON, T. W. (and G. C. MARTIN). Mesozoic Section of Cook’s Inlet and Alaska Peninsula. (Bull. Geol. Soc. Am., vol. 16, pp. 391-410, Pls. 67-70, 1905). STEIGER, GEORGE. The action of silver nitrate and thallous nitrate upon certain natural silicates. (U.S. G.S. Bull. No. 262, pp. 75-91, 1905). STEIGER, GEORGE. (See CLARKE, F. W.) TAFF, J. A. Progress of coal work in Indian Territory. (U.S. G. S. Bull. No. 260, pp. 382-402, 1905). TAFF, J. A. (and M. K. SHALER). Notes on the geology of the Muscogee oil fields. (U.S. G. S. Bull. No. 260, pp. 441-446, 1905). TAYLOR, T. N. (and J. C. HOYT). Progress of Stream Measurements. (U.S. G. S. Wat. Sup. and inte eaAD eNO: loasebart.g, DD. Los, DIS. 2, 1905): TRUE, F. W. A Fossil Sea Lion from the Miocene of Oregon. (Smithsonian Misc. Coll., vol. 3, pp. 47-50, 1905). UDDEN, J. A. On the Proboscidean Fossils of the Pleistocene Deposits in likinois and Iowa. (Augustana Lib. Pub. No. 5, pp. 43-57, 1905). ULRICH, E. O. (and W. S. TANGIER SMITH). The Lead, Zinc, and Fluorspar Deposits of Western Kentucky, Part I. (U.S: G. S: Prof. Pap. No. -36, pp. 104, Pls: 7, 1905): IQA). - The American Geologist. September, 1905 UPHAM, WARREN. Geological History of the Great Lakes and Niagara Falls. (The International Quarterly, vol. 11, pp. 248-265, July, 1905). VERMEULE, C. C. . East Orange Wells at White Oak Ridge Essex County. (Geol. Sur. of N. J., Ann. Rep. 1904, pp. 253-263). WEED, W. H. Foreign Copper Mines. (Mining Mag., vol. 12, pp. 5-18, July, 1905). WELLER, STUART. The Fauna of the Cliffwood Clays and the Classification of the Upper Cretaceous Formations and Fauna of New Jersey. (Geol. Sur. N. J., Ann. Rep. 1904, pp. 131-145). ) WHITE, CHAS. A. The Ancestral Origin of the North American Unionide, or fresh- water Mussels. (Smith Misc. Coll., vol. 3, pp. 75-89, 1905). WHITE, C. A. The Relation of Phylogenesis to Historical Geology. (Science, vol. 22, pp. 105-113, July 28, 1905). WRIGHT, G. FREDERICK. Recent date of Lava flows in California. (Records of the Past, vol. 4, Part 7, p. 195, July, 1905). WRIGHT, G. FREDERICK. Albert A. Wright. (Am. Geologist, vol. 36, No. 2, pp. 65-69, Aug., 1905). CORRESPONDENCE Notes on Fossits OBTAINED AT SANKATY HEAD, NANTUCKET IN Juty 1905.—Through the kindness of members of the Nantucket Maria Mitchell Association I was fortunate enough to make a suc- cessful collecting trip to the exposure at Sankaty Head in July of the past summer. By the united efforts of the party a section through the fossiliferous beds was laid bare and then worked systematically. The results of the collecting in this manner and also by looking over the loose material were very gratifying. The ~ material thrown out in the previous year’s excavating by Mr. J. Howard Wilson was well worked over by the rains of the previous winter and spring. In the small gullies at the base of this material small shells and crab claws were easily seen although very hard to see in the freshly exposed material. As a result of this search- ing a considerable number of small shells and crab claws were obtained. Correspondence. 195 One of the finds here was a single specimen of Scala , Making the first specimen of this species known from these deposits. The specimen was excellently preserved. A single specimen of Scala groenlandica Perry, was found here many years ago and was noted in the writer’s’ previous list of the Sankaty Head fossils. Another svecies of interest was Cerithiopsis green C. B. Adams, of which but very few specimens have been found at this locality. This specimen was also excellently preserved, showing the. proto- conch complete. Among the smaller shells collected were several species of Odostomia. Of these the two species previously reported from Sankaty—Odostomia impressa Say and O. trifida Gould,—were the most common, the former being represented by at least three times as many specimens as the latter. Besides these two species there were found O. fusca C B. Adams, O. bisuturalis Say, and O. semi- nuda C. B. Adams. These three species have not:previously been reported from Sankaty. Among other things of interest was the finding of Arca pon- derosa Say in situ, both valves being together and in the position of life. This species was previously known from this locality by a single valve found by the writer among the material collected by Dr. Scudder. Other pelecypods were found in the lower layer with both valves attached and the shell in the natural position. This tends to show that. the shells of this layer at least are in situ and not secondarily deposited. The crab claws collected included three species. They were identified by Miss M. J. Rathbun as Callinectes sapidus Rathbun, Eupanopeus herbstii Milne Edwards and Neopanope texana sayi Smith. Tae last was much-more common than either of the other species. In the collection at Nantucket were found two other species of very considerable interest as they were unknown from this locality at the time of publication of the former list (Am. Geol. vol. xxxiv, Sept., 1904). These inciude a specimen of Sipho stimpsoni Morch, with an excellently preserved protoconch and a large speci- - men of Chrysodomus decemcostatus Say. This latter is a fairly complete specimen, part of the body whorl being broken away, but the spire in good shape. JosEpH A, CUSHMAN. Boston Society of Natural History, September, 1905. FIELD GEOLOGY IN OHIO STATE UNIVERSITY. Each spring term an elective course in Field Geology is offered by professor Prosser for advanced undergraduate and graduate students. The purpose of the course is to acquaint the student with the formations as they are seen in the field and to train him in the methods of investiga- tion employed by the working geologist. The course consists of field excursions, laboratory work and study of library references. 196 The American Geologist. Sepeaue oer In the field the formations are carefully studied, identified and measured preparatory to making sections and writing detailed descriptions which ultimately take the form of a thesis. In the laboratory, characteristic fossils of the various formations are identified and the literature of the region under investigation care- fully studied. Last term fifteen students registered in this course, two of whom were girls, and the latter were as energetic and en- thusiastic as the men. The usual equipment for the trips consisted of barometers, hand-levels and staff, tape lines, hammers, chisels, collecting bags and camera. A trip was made each Saturday dur- ing the term, with one exception, although the spring was un- favorable for field work on account of the frequent and heavy rainstorms. Ohio state university is well situated for geological work since every formation of central Ohio is readily reached by one or more of the numerous steam or electric railways radiating from’ Colum- bus. Every formation of the state from the Richmond to the Alle- gheny inclusive was studied in the field save the local and rela- tively unimportant Hillsboro sandstone. The distance traveled aggregated about 500 miles. The longest and most interesting trips from the standpoint of stratigraphy and paleontology were to Zanesville in Muskingum county and to Waynesville in Warren county. The latter occupied two days and included trips to the beautiful gorges at Cedarville, Clifton and Yellow Springs. Goe’s Station to the south of Yellow Springs was also visited, at this time, where the mottled clays of the Saluda, the Belfast bed and Clinton limestone are excellently shown in a small ravine near the former residence of Mr. Goe. The heavy rains had thoroughly washed all of the small gullies on the hillside and the mottled clays of the Saluda were shown at their best. All of the sub-divisions of the “Niagara” of Ohio, with the exception of the Hillsboro sandstone, were studied at Yellow Springs, Clifton and Cedarville. The Osgood or Niagara shale is best exposed on the bank of Cascade glen at Yellow Springs, while farther up the stream are outcrops of the West Union, Springfield and Cedarville limestones. The gorge of the Little Miami river below Clifton is famous as one of the most picturesque localities in southwestern Ohio, its banks formed by the Springfield and Cedarville limestones. On Massie’s creek, however, a little below Cedarville is a vertical cliff which is one of the most interesting places in this region since it shows the contact of the Osgood shale and West Union limestone, the entire thickness of the West Union and its contact with the superjacent Cedarville limestone. In this vicinity is a most clearly marked old channel of the creek, the bed of which is now dry and covered with grass. The Monroe forma- tion, or Waterlime of the Ohio reports, occurs to the west of Columbus and one day was devoted to the study of several of its outcrops which involved a tramp of some twelve miles. The Personal and Scientific News. 107 Devonian limestones and shales are excellently exposed on the Scioto river and its tributaries and the various formations of the Waverly series on the streams to the east of Columbus within a distance of from ten to thirty-five miles. All of these formations were carefully studied using for a guide the recent papers of professor Prosser in which they have been fully described. The youngest Carboniferous formations studied were seen at Zanesville, sixty miles east of Columbus, where the Lower Mercer limestone occurs in the bed of the Muskingum river, and Putnam Hill and the adjacent ones show the succeeding members of the Pottsville and Allegheny formations as high as the Freeport sandstone. 2 GEORGE F. Lams. PERSONAL AND SCIENTIFIC NEWS. WER). SPURR of the U.S. Geol, Sur. has resigned:to accept a position with the Guggenheim Exploration Co. Mr. Spurr has been connected with the survey for ten years and was previously with the Minnesota Geol. and Nat. Hist. Survey. He has written reports on the Mesabi range, the Mercur, Aspen, Monte Christe, Klondyke and Tonopah districts and was to have studied the Goldfield district this year. His work there will be taken up by Mr. F. L. Ransome. WE ARE GRATIFIED TO LEARN that we have been misin- formed in regard to a change in the geological survey of Michigan.—Dr. A. C. Lane is still the able director of that survey. During the present season much active work is going on. Professor Russell is making an examination of the surface geology in the Upper Peninsula, and Mr. Frank Leverett of the United States survey is on the same problem. They are working in cooperation. And at the same time professor C. A. Davis of the university is studying the de- velopment and ecology of the peat bog flora. Mr. W. C. Gordon is completing a careful cross section of the copper- bearing formation, to determine the different horizons, near the Wisconsin line. Professor W. M. Gregory is finishing his report on Arenac county. Mr. W. F. Cooper is working on the Wayne county report and watching the shaft going down to rock salt, near Detroit. The state geologist is en- gaged in detailed studies in the copper region. SINCE THE RECENT REORGANIZATION of the Louisiana Survey two volumes have been published on the geology of the state, and are known generally as'the “Report of 1899” 198 The American Geologist. Septemberslaa and the “Report of 1902.” In preparing the “Report of 1905” it has seemed advisable owing to the diversity of subject matter, to publish the same in parts and, as usual, style such parts “Bulletins.” Bulletin No. 1—Underground Waters of Louisiana; Bulletin’: No. 2—Magnetic Survey of Louisiana; and Bulletin No. 3—Tide Gage Work in Louisi- ana, have already been published and may be had gratis by addressing Dr. W. R. Dodson, director Experiment Sta- tion, Louisiana, at Baton Rouge, La. For the reports of 1899 and 1902 address “Director Sugar Experiment Sta.,” Audubon Park, New Orleans, La. STUDENTS IN THE INTERCOLLEGIATE summer field course in the geology of the Appalachian region spent the first week in studying the formations of the Coastal Plain of Maryland under the direction of Dr. Clark of Johns Hopkins univer- sity and Dr. Miller of Bryn Mawr college. Professors Bib- bins of the Woman’s college of Baltimore, Cleland of Wil- liams college and Westgate of Ohio Wesleyan university were also members of the party. The boat of the city en- gineer of Baltimore and the private yacht of the governor of Maryland were generously placed at the disposal of the par- ty which greatly facilitated the work. The second week under the direction of professor Davis of Harvard was spent in central Pennsylvania in studying the Appalachian struc- ture and physiography. Professors. Cleland, Westgate, Prosser of Ohio State university and Rice of Wesleyan uni- versity of Connecticut participated in this work. The third week was spent studying the formations of central New York, with headquarters at Syracuse, under the direction of professor Hopkins of Syracuse university. From Wed- nesday to Saturday of this week Section E of the American Association for the Advancement of Science was in session at Syracuse and the following well known geologists partici- pated in some of the excursions: Rice, Prosser, Taylor of Indiana, David White of the U. S. Geol. Sur., Hovey of the American Museum of Natural History, Fairchild of Roches- ter university, Cushing of Western Reserve and Grabau of Columbia university. The party left Syracuse Saturday with professor Cushing who directetd the study of the pre- Cambrian crystalline and Ordovician formations of the Mo- hawk valley during the fourth week of the course. THE meric AN GEOLOGIST. VOL. XXXVI, OCTOBER, 1905. No. 4. TEN YEARS PROGRESS IN THE MAMMALIAN PALAZEONTOL- OGY OF NORTH AMERICA.* By Pror. HENRY FAIRFIELD OsBorRN, LL. D-, D Sc., New York. Members of the Congress, I believe that what you as specialists in the many di- verse branches of zoology most desire to hear, are the salient results of our recent explorations in America, and their broader bearings on the general principles of zoology. In 1878, the late professor O. C. Marsh published his notable address entitled: Jntroduction and Succession of Vertebrate Life in North America’. Fifteen years later [ published a somewhat similar review entitled: ase of the Mammalia in North America’. In the ten years which have elapsed exploration has not only been on a larger scale* than ever before, but also more thorough as well as guided by the constantly broadening aspects of the science. The initial plan of the paleozoological survey under- taken by the American Museum was threefold: it was so far as possible to secure-not only (1) a complete representation of certain families of mammals, as was done for mono- graphic purposes by Marsh (i.e. Dinocerata, Brontotheriidz) * Address of Prof. H. F. Osborn at the International Congress of Zoo- logy, Berne, August, 1904. Reprinted from the Compte-Rendu of the Congress by permission of the secretary. 2 Proc. Arner. Assoc. Adv. Sci., Nashville, 1877, pp. 211-258. 3 Amer. Jour. Sci. 18, xlvi, 1893, pp. 379-392; 448-466. 4 Large collections have been secured by the Museums of Princeton University and the University of California, by the Carnegie Museum Pittsburgh, the Field Columbian Museum, Chicago, and some few addi- tions nave been made to the famous collection brought together by professor MarsuH at Yale University. ‘The Department of Vertebrate Palaeontology in the American Mu- seum of Natural History was founded with the present writer as Curator in 1891. Associated with him at various times were the following zoolo- gists and palaeontologists: Messrs. WortMAN, MATTHEW, EARLE, GIDLEY and Brown. ‘Fossil mammals brought from the West, secured by ex- change, and by purchase, including the entire collection of the late professor Edward D. Cope, now number 9873. The Copa Reptilian and Amphibian Collection is also in the American Museum, 200 The American Geologist. October, 1905 (2), 2 complete representation of certain contemporary faunas, as was done chiefly by the late professor Edward D. Cope (e. g. the Puerco and John Day faunas), but in addition (3) to secure complete phyletic series of various families of mammals in successive geological horizons from their intro- duction to their extinction (compare Fig. 2). In each of these features of our plan we have been rewarded with a success far beyond our most sanguine expectations. Our large collections studied by friendly cooperation in connec- tion with those of other institutions, and large collections studied independently in other institutions, notably Prince- ton and the Carnegie Museum, have naturally brought into a new light some of the important general principles of palzozoology. I. Progress in the General Principles of Paleozoology. Palwogeography—vThe first broader bearing is that of past distribution and paleogeography, in which the accuracy of our records! and thoroughness of our search are working a revolution. We are finding the remains of animals which have recently arrived from South America, Asia, Europe’ and Africa®, and it would be impossible to narrow the field of American fossil mammalogy even if we desired to do so. The broad study of intercontinental evolution and relations of the mammals is absolutely essential to a philosophical understanding. Those who have followed the rapid recent progress of paleontology ,know that this spirit of uniting paleontology ever more closely with distribution and paleo- geography is that which constantly animates the older as well as many of the younger workers in this field. Zoological methods—Zoology in the sense of studying’ extinct forms as living organisms is also becoming closer day by day, and we are now enjoying the recognition by mammalogists (Weber!, Beddard’) of the absolute necessity of coupling the study of ancestral with that of the recent forms in all questions both of distribution and of classifica- 1 MattHew, W. OD. A Provisional Classification af the Freshwater Tertiary of the West. Bull. Amer. Mus. Nat. Hist., vol. xii, 1899, pp. 19-77. 2 Osporn, H. F. Faunal Relatians of Eurone and America during the Tertiary Period. Ann. N. Y. Acad. Sci., vol. xiii, 1900, pp. 46-56. 3 OsBoRN, JI. F. Theory of Successive Invasions of an African Fauna into Europe Ann. N. Y¥. Acad. Sci., vol. xiii, 1900, pp. 56-58. 1 Die Saugethiere 8°, Jena, 1904. 2 Mammalia. The Cambridge Natural History, 8°, 1902. Progress in Mammalian Palaeontology. 201 tion. In connection with distribution our chief advance has been to determine the exact geographical location and chronological succession of animals, the local conditions of geological deposition in relation to habits and habitat or en- vironment, as well as its bearing upon the study of past cli- mates, or what may be called paleometeorology. Adaptive radiation, continental—In connection with the comparison of mammals in their intercontinental as well as im their continental relations, the branching system of Lamarck and the divergence which impressed Darwin is perhaps most clearly expressed by the word “radiation’”. Elsewhere the conception of adaptive radiation has been fully developed in connection with the origin of certain orders’. - It may here be briefly pointed out that Africa’, South America, North America and Eurasia prove to have been the three chief geographical centres of ordinal radiation. Adaptive radiation, local.—Quite as important, al- though not carried on so grand a scale, is the local adaptive radiation which brings about a diversity of type in the same geographical regions and is the basis of the polyphyletic law of which we shall next speak. It is perhaps best illustrated by the Ungulates. In addition'to (1) digital reduction (Kowalevsky) and (2) carpal and tarsal displacement (Cope, Osborn) in relation to the choice of harder and softer ground, there is recognized (3) after the primary con- version of semi-unguiculate into ungulate types, a reversed conversion of ungulate types into clawed types, as seen in Dichobune (Artiodactyla), Chalicotherium (Perissodactyla), and perhaps in an incipient stage in Agriochoerus (Artiodac- tyla) ; (4) secondary adoption of aquatic habits, as seen, for example, in the Amynodontidze among the Rhinocerotoidea. Divergence by the above factors has long been recognized. There are also to be seen phyletic series combining in vari- ous ways either of. the following eight conditions of foot, 3 OsBoRN H. F., Rise of the Mammaiia. Proc. Amer. Association, Adv. Sci., vol. xlii, 1893, ». 215. 4 Adaptive Radiation of Orders and Families Ann, NW. YY. Acad: Set vol. xiii, 1900, nn 49-51. 5 Ann. N. Y. Acad. Sci. xiii, 1900, pp. 56-58. 6 OsBorn, H. F.. The Law of Adaptive Radiation. Amer, Nat. xxxvi, 1902, pp. 353-363. 202 The American Geologist. October, 1905 skull and tooth structure, which are not found to be neces- sarily correlated: Primitive Condition. Secondary Condition. (6) Elongation (dolichocephaly ) of skull (7) Abbreviation (brachyceph- aly) of skull (5) Mesaticephaly (9) Elongation (dolichopody) of limbs (10) Abbreviation (brachypody of limbs (8) Mesatipody (12) Elongation (hypsodonty) of (11) Brachyodonty { uate Law of correlation.—The bearing of these observations on Cuvier’s law of correlation is to modify rather than to displace it. It may be restated as follows!: The feet (cor- related chiefly with limb and body structure) and the teeth (correlated chiefly with skull and neck structure) diverge independently in adaptation respectively to securing (feet) and eating (teeth) food under different conditions; each evolves directly for its own mechanical functions or pur- poses, yet in such a manner that each subserves the other. Thus, for example, there is a frequent correlation between dolichocephaly, dolichopody and hypsodonty, as in certain of the Hguidae, but there are so many exceptions to such correlation, because of the separate adaptive evolution of each organ, that it would be entirely impossible to predict the structure of the tooth from the structure of the claw, or vice versa, Law of analogous evolution. —One of the most impor- tant advances of the past decade, for which the way was largely prepared, in the previous decade, by Scott’s papers on Oreodon, Poebrotherium and Mesohippus, has been the clear recognition of this law. These phenomena give rise to an enormous number of analogies (homoplasies, parallel- isms, convergences) not only of structure but of entire types, of families, and of groups, very confusing to the seeker of real phyletic relationship. 1 Osborn. Amer. Nat. xxxvi, 1902, p. 363. Progress in Mammalian Palaeontology. 203 Evolution in part determinate. —As regards the modes and factors of evolution’, the continuous stages of evolution which we are securing among the horses, camels, rhinocer- oses, and many other families, afford opportunities which havé never been afforded before. We are with adaptive characters from their birth or genesis, through their prime, into their decline and death. Through this unique oppor- tunity for observation has been confirmed a view of evolu- tion long shared by most if not all paleontologists, verte- brate and invertebrate, but naturally not understood or | PRINCIPAL FORMATIONS IN WHICH FOSSIL ae Es ARE FOUND IN WESTERN UNITED STATE CHARACTERISTIC | CORRESP EUROP EUROPEAN PUMMALS| FORMATIONS CHARACTERISTIC AMERICAN MAMMALS GREAT PLAINS SECTION Equus slenomis | var pe macarnre ipparion pantera) ORECON, SECTION_| A ABS CAL MIOCENE iii 1 v |Anchitheriurn |O*'6 7 “84N | SAN SAN | Mastodon SABLES DE CORL Diceratherium Ba SE RANT SE ie Protchippus Hala therwarn Titanotherium al Ta ips Epthippus | Coryphodon |Lower ie MONTANA SECTION _.... - Eohippus CERNAYSIEN uprologona TcuK0n |BASAL HY aie BNTONA i CACC.GROS DE Mons > = UNION: (Ae ne le Palyrmastoden | CRETACEOUS Dinosauric) FIG 1 Most recent geological subdivision of the American Tertiary. Showing that the successive sections in Montana, New Mexico, Wyo- ming, Utah, Oregon, and the Great Plains afford a complete history of the Tertiary, homotaxial with that afforded by the corresponding Euro- pean formations. 3! d by otl zoologists hk se of tl ssentially differ- Snared Dy other zoologists because oO 1e essentia y aiirer ent nature of evidence. I refer especially to the theory of 2 Scorr, W. B. On the Mode of Evolution in the Mammalia and on some of the Factors im _ the Evolution of the Mammalia. Jour. Morphol. vol. v, 1891, No. 3, pp. 361-378, 378-42. 204 The American Geologist. October, 1905 the definite or determinate ‘origin! and development of cer- tain at least of the new adaptive structures, apparently, but not certainly according to the principle to which Waagen applied the term mutation’. The mutation of the palzon- tologist, however, is quite distinct from the phenomena of minute saltations to which de Vries has applied Waagen’s term in his valuable experiments}. Potential of similar evolution—In connection with ana- logous, but especially with partially determinate evolution, we not only have the similarly moulding influences of simi- lar habits, and the action of the various factors of evolution” which we cannot stop to discuss, but clear evidence of the existence of a potential of similar evolution, a kind of latent homology which determines that when certain structures are to appear among animals independently derived from a common stock, they will appear at certain definite points and not at random. For example, the genesis of the rudi- ment of the horn in three independent phyla of Eocene titan- otheres is at exactly the same point, namely, at the point of junction of the frontals with the nasals at the side of the face just above the eye. The polyphyletic law.—Partly as an outgrowth of the synthesis of the above principles and partly as the result of new discoveries and the closer study of types already known is the full recognition of the polyphyletic law.’ If we ex- amine the phylogenies of Huxley and Cope, and even those of more recent writers (Scott, Osborn, Wortman) of a decade ago, we find that the attempt is made for example, to trace the pedigrees of the horses and rhinoceroses in a monophyletic manner. The first known instance of this kind was Huxley’s pedigree of Aguus through [ipparion, Anchi- therium and Palaeotherium, all of which are now known to belong to entirely distinct phyla. Another instance was 1 OsBorN, H. F. The Falaeontological Evidenec for the Transmission of ; Li 2 Paniotestes ? Panloles lis 3 FIG. 5. The Polyphyletic Law and Local Adaptive Radiation Illustrated in the Phylogeny of the Camels. On the left is illustrated the older monophyletic view held as recently as 1898; on the right, the newer polyphyliletic view developed in 1904 show- ing three distinct contemporary lines of Camelidae. fluviatile or channel beds, with chiefly lowland or bottom fauna, from eolian or backwater sediments, chiefly with a plains and cursorial fauna. The three subdivisions origin- ally observed by Hayden and Leidy are thus divided follows: I. Fluviatile or Channel Beds. IJ. olian or Backwater Sediments. Wpper; Protocerasibeds: 0. >... .. Leptauchenia beds. Middle, Metamynodon beds....... Oreodon beds. Lower, Titanotherium beds. This separation was chiefly brought about by Matthew’s careful analysis of the animals coming from these respective 218 The American Geologist. October, 1905 beds, the former (1) including lowland, forest and river- bottom, and aquatic animals, the latter (II) the animals of the plains and uplands. The John Day beds of Oregon apparently contain an overlapping fauna partly equivalent to the Upper Oligocene and partly to the Lower Miocene. The already well known (Cope, Filhol) and close zoogeographical relationships during the Oligocene of North America and Europe are strengthened by the discovery of European Anthracotheriide, Mustelide (Bunaelurus') and Erinaceide (Proterzw, Matthew’) in America, and of the American Titanotheriide in Europe’. This leaves as the chief families in Europe still unknown in America the Paleotheriide, Anoplotheriide, Tragulide. Our faunal knowledge has been especially enriched by the discovery and description of the hitherto unknown microfauna of the Titanotherium beds (Douglass*, Matthew’) which includes archaic, Centetes-like forms, as well as Hrin- a ceous -like forms. The main phylogenetic results are the following. The Creodonta have been definitely traced to their extinction in the Hyznodontide (Table II). Among the Canidz the an- cestral line of Cyon (Dholes) has almost certainly been recognized in this period in the genus Zemnocyon (Wort- man and Matthew®) (Fig. 6). No trace of Edentata has been found, the forms formerly described as such now being known to be the peculiar Chalicotheriidz, probably of Peris- sodactyl affinities. The rhinoceroses have been traced back in the Lower Oligocene to animals (Zrigonias) with sev- eral incisors as well as with canine teeth (Osborn!, Lucas’). 1 MarTrHew, W. D. On the Skull of Bunaelwrus, Bull. Amer. Mus. Nat. Hist., xvi, 1902, pp. 1387-140. 2A Fossil Hedgehog from the American Oligocene Bull. Amer. Mus. Nat. Hist., vol. xix, 19038, pp. 227-229. 8 TouLta. Ueber neue Wéirbelthierreste aus dem Tertiar Oe6esterreichs und Rumeliens, Zeitschr. d. Deutsch. geolog. Ges., Jahrg. 1896, pp. 922-924. Foss. Mamm. White River. Trans. Amer. Philos. Soc, n. s., vol. xx, 1901, p. 1-42. ; 5 The Fauna of the Titanothertum deds. Bull. Amer. Mus. Nat. Hist., vol. xix, 1908, pp. 197-226. 6 Bull. Amer. Mus. Nat. Hist., vol. xii, 1899, pp. 139-148. yale Extinct Rhinoceroses. Mem. Amer. Mus. Nat. Hist., vol. i, 1898, po. 75-165. “ ae New Rhinoceros, Trigonias Osborni. Proc. U. S. Nat. Mus. xxiii, oO. 1207. Progress in Mammalian Palaeontology.—Osborn. 219 The law of local adaptive radiation with its polyphyletic consequences has completely altered our conception of sev- eral Oligocene families, as follows. The Titanotheriide (Osborn*®) break up into four genera, which evolve inde- pendently from the base to the summit of the Oligocene, namely, Zitanotherium, Megacerops, Symborodon, and Bron totherium,; divergence is indicated by dolichocephaly and brachycephaly as well as by other characters (Fig. 7). Sim- ilarly the Equide break up into four and possibly five dis- tinct contemporary phyla, and it now begins to appear prob- able that the line giving rise to Equus, separated off from the other horses as early as the Lower Oligocene (Osborn, Gidley; Fig. 4). The Oreodontide, represented by two phyla in the Upper Eocene, now present three phyla, name- ly, Agriochoerus, Oreodon, Leptauchenia (Matthew). Three phyla of Camelidz are also recognized, namely, those repre- sented by Paratylopus, Poebrotherium, and Pseudolabis (Matthew, Fig. 5). Similarly among the Felidz, the Mach- erodont division, the only felines represented in America at this time, breaks up into the stout-limbed Hoplophoneus series ancestral to Muachaerodus and Smilodon the slender- limbed Dinictis *, and a third series represented by Vimravus (Fig. 6). Among the gaps in the Oligocene is the entire absence of Primates, the genera Laopithecus and Menotherium, for merly associated with the Primates, proving to be singularly primitive tritubercular Artiodactyls. An important prob- lem is the actual relationships of the Artiodactyl genera Pro- toceras, Leptomeryx, Hypertragulus, and Hypisodus, which according to Scott’s theory above alluded to, represent with the Oreodontidz an independent radiation of American Arti- odactyla wholly without affinity with the European Tragu- lines. Toe Miocrnrt Fauna. In our Miocene, equivalent to the Langhien (Orléanais), Helvétien (Sansan, Simorre), and Tortonien (Grive St. Al- ban, Bamboli) stages of Europe, the most exceptional pro- 3 Bull. Amer. Mus. Nat. Hist., xvi, 1902, pp. 91-109. . 4 MatrHew. Fossil Mammals of the Tertiary of Northeastern Colorado Mem. Amer. Mus, Nat. Hist., vol. i, pt. vi, 1901. 220 The American Geologist. October, 1905 gress has been made in the distinction of the geological and faunal zones. Ten years ago the accurate geological ob- servations of Hayden were overlooked, and it was believed that formations equivalent to the Middle and Lower Mio- cene of Europe were sparsely if at all representetd. Now three faunal stages are clearly recognized (Scott!, Matthew’, Gidley’), namely: Lower (Rosebud beds), in which the ani- mals are still sparsely known, Middle (Deep River beds), in which the fauna is becoming more fully known, Upper (Loup Fork beds), in which a very rich fauna is now fully known. Each of these divisions is distinguished by specific stages in the evolution of the horses, rhinoceroses, camels, oreodonts, rodents, and carnivores. These chronological successions derived from geology have already yielded very important new biological results. The zoogeographical relationships with Europe have been strengthened by the discovery for the first time of Din- ocyon ( Matthew’), of a new species of rhinoceros ( Zele- oceras bicornutus* Osborn), closely similar to the Zvleoceras aurelianensis of the Lower Miocene of France, by the rec- ognition of new Mustelide (Lutra), and of the Castoride (Dipoides). The Proboscidea, now known to be of African origin, are not certainly found in the lower and sparsely known in the middle, but are fully represented in the upper beds. In the middle beds appears JMastadon productus, rather derivable from the Palaeomastodon of Africa than from the AL. angustidens of France. Our views as to the ‘Miocene climate have also under- gone a change, owing to the recognition that most of these deposits are fluviatile and zxolian rather than lacustrine (Matthew, Gidley’), as evidence of a dry climate, marshy 1 The Mammalia of the Deep River Beds, Trans. Amer. Philos. Soc., XVili, 1895, pp. 55-185. 2 Foss, Mamm. of the Tertiary, etc. Mem. A. M. N. H., vol. i, 1901. 3 New or Little Known Mammals from the Miocene. Bull. Amer. Mus. Nat. Hist., xx, 1904,. pp. 241. 1A Skull of Dinocvon from the Miocene of Texas. Bull. Amer. Mus. Nat. Hist., vol. xvi, 1902,> pp. 129-136. 2 New Miocene Rhinoceroses. Bull. Amer. Mus. Nat. Hist., vol, xx, 1904, pp. 307-326. 3 New or Little Known Mammals from’ the Miocene eof South Dakota Bull. Amer. Mus. Nat. Hist., vol. xx, 1904, pp. 241-268. RECENT PLIOCENE, % fe. - OLIGUENE One. (reef Vapor 6 Mund le ' GOcenE Progress in Mammalian Palaeontology.—Osborn, 221 PROVISIONAL PHYLOGENY OF CARNIVORA, OLD &NEW WORLD.’ “WO Matthew oye i FELIDAE MUSTELIOAE VINERRIDAE HYAEMIDAE CANIDAE FRECTON- UR. —— te — a oo Prod selort tT eateiheanes Dinietio aba rage! “9 ese ae ae oT plant Dimes 5? y Aglorogele 4 ora lus * Diacshe 7 Phendachures/ Steno > Y ar %, if o a ee J AEs Fy “s ie aoa J ) Zz sid ; a rigaiall y a 3 wv. Z america i - owe a www @ - -_—— - 2 oy ae ee oe ‘fe ae ‘\ Vivarranas | aa Supope . . ~ ane pd ee FIG. 6. The hypothetical phylogeny of the Carnivora illustrating especially the great antiquity of some of the modern genera of dogs, such as Cyon, which separated off from the other Cranidae in the base of the Oiigocene if not in the Eocene. This table includes also the European Carnivora and is of a temporary value. /Falaeonictis, although a Creo- dont may possibly be related to the Felidae. plains, and drifting sands, rather than of the moister climatic conditions inferred from the older lake basin theory. Among the chief phylogenetic results are the addition of at least four kinds of Canids (Fig. 6) and the tracing back of the Procyonide to the Lower Miocene Phlaocyon ( Matthew’), tending to unite this phylum more closely with the Canide. The Mustelide are now represented by Mus- tela and Lutra. The Viverride and Ursidz are still wholly unrepresented in Arrerica although evolving contemporane- ously in Europe. Among the distinctively American Artio- dactyls the Cervide are now recorded in the Middle Mio- cene ( Palacomeryx), a fact however still requiring confirma- tion. In this connection should be mentioned the discovery of the full characiers of the genus Merycodus ( Cosoryz), 4 Foss. Mamm of the Tertiary, etc. Mem. A. M. N. H., vol. i, 1901. 222 The American Geologist Oe aee Oe which with Blastomeryx as the new family Merycodontide has been regarded by Matthew’ to be more nearly related to the American Antilocapride than to the European Cervi- de, although its deerlike horns certainly suggest Cervine relationships. The Camelide until recently considered monophyletic have bcen shown to be in a marked degree polyphyletic®, the Lower Oligocene Paratylopus giving rise to two phyla, one of which includes the “giraffe camel,” Alticamelus (Matthew!), which presents a remarkable anal- ogy in the elongation of its neck and limbs with the giraffes of Africa; similarly Proebrotherium splits into three phyla (Fig. 5, Matthew). Similarly the Oreodont, and Agrichcerine phyla have disappeared without leaving successors. The rival cursorial Hyracodontide and aquatic Amynodontide having died out, the true Rhinocerotide (Fig. 3) split up into three series, one including the extremely long-skulled and long- limbed types, possibly related to the true Aceratherium in- cisivum of Europe, a second including excessively broad- skulled types (genera Aphelops and Peraceras Cope), and a third including the short-footed (brachypodine) types ( Teleoceras ), almost certainly of European origin. The Tapiride are still sparsely known. The aberrant Chali- cotheriide terminate *in an Upper Miocene species which nearly equals in size the Lower Pliocene Ancylotherium of the Pikermi. The most astonishing discovery among the Rodentia is that of a member of the Mylagaulide with a very large horn core on the front portion of the skull genus Ceratogaulus Matthew’). The principal work still to be done in our Miocene is the following: to ascertain more fully the character of the Lower Miocene fauna, which is still unknown; to fix the date of the arrival of the earliest Proboscidea either early in the Middle or in the Lower Miocene; to trace the ancestry of the typical dogs; to ascertain the origin of the Cervide, which will probably prove to be Asiatic, as well as the origin of the peculiarly American Antilocapride. 5 A Complete Skeleto of Merycodus. Bull. Amer. Mus. Nat. Hist., vol. xx, 1904, pp. 101-129. : 6 Notice of Two New Oligocene Camels, Bull. Amer. Mus. Nat. Hist., vol. xvi, 1902, pp. 617-635. ; eae: Mamm. of the Tertiary, ete. Mem. A. M. N. H., vol. i, pt. vi, ; Progress in Mammalian Palaeontology.—Osborn. 223 Tue Priocrene Fauna. Equivalent to Messinien (Pikermi), Plasancien (Cas- ino), Astein (Rousillon), Sicilien (Val d’ Arno sup.) Our limited American Pliocene fauna still stands in sad contrast to the rich succession of Pliocene mammals of Europe. The Palo Duro mammals which Cope included in the Pliocene have proved to be Upper Miocene. Recent geological and paleontological work (Gidley’) shows that the only true Pliocene formation and locality is that of the Blanco beds of Texas, 75 feet in thickness, as against the rich successive Pliocene series of Europe. Nor are any species of Hguus found here, as Cope supposed, and as might be expected from the presence of Aguus (££. stenonis) in the Upper Pliocene of Europe. The chief faunal distinc- tions are the entire disappearance of the Rhinocerotidz and the appearance of South American Mammals. The zoogeographical changes are well known to enter a new relation by the invasion of the South American Edenta- ta, namely, Glyptodon, Megalonyx, Mylodon. Among these anew Glyptodont, Glyptotherium texanum has recently be- come known (Osborn!) from a nearly complete carapace and partial skeleton, which exhibits primitive affinities with the Eocene types of Patagonia. Among the Proboscidea the Stegodont stage appears in the so-called Mastodon mir- ficus of Leidy, indicating a late Pliocene age for the Blanco formation. In the marine Miocene of Japan (Iwasaki and Yoshiwara’) the remarkable discovery has been made of an anomalous skull representing a new family (Desmostylidae fam. nov.) either of hypsodont Sirenia or of Proboscidea, and Merriam! has recognized as a similar form occurring on the coast of California the genus Desmostylus first noticed by Marsh. The phylogenetic series is all too limited, the horses 2A Horned Rodent. Bull. Amer. Mus. Nat. Hist., voi. xvi, 1902, pp. 291-310. 8 The Freshwater Tertiary of _ Northwestern Texas. Bull. Amer. Mus. Nat. Hist., vol. xix, 1903, pp. 617-635. 1 Ghyptotherium texanum Bull. Amer.. Mus. Nat. Hist., xix, 1903, pp. 491-494. 2 Notes on a New Fossil Mammal. Jour. Coll. of Sci. Imp. Univ. Tokyo, vol.’ xvi, Art. 5, 1902. 1 Science, n. s., vol. xvi, Oct. 31, 1902, p. 714. Di vergent Characlers ‘ The American Geologist. October, 1905 LAW OF LOCAL ADAPTIVE RAD/AT/ION Conremporary Evocurion of Four Purea of Tiraworneres , Lower Oxicocene , Nort Amenica BRACHYCEPHALIC MESOPODAL SHORT HwORWS iNCISOR TEETH OOLICHOCE PHALIC OOLICHOPIDAc SHORT HORNS, NO INCISOR TEETH BRACHYCEPHALIC LONG NARROW HORNS WO INCISOR TEETH ~ MESATICE PHALIC MESOPOOAL LowG BRoAD Hwokns } INCISOR TEETH MEGACEROPS TITANOTHERIUM SYMBORODON BRONTOTHERIUM ° B platyceras M. robustus B ramosum Ay S..acer Upper : ‘Beds M-dispes M.bicornulus AB: dolichoceras B.gigas q A serotinus F * Middle» JT. trigonoceras : 4B hatchere Beds. | Lower ~ jBede |M. Wap Uf helocera’s % = 4 Collaleral } lines ib D reel dine Collateral lines A al Divect Collateral | Direct Collateral Tolel thick- \ line line dines: mess, 180 fl Me m e co SSHORT HORNED ‘TITANOTHERES lines LONG HORNED TITANOTHERES FIG. 7. of local adaptive radiation illustrated in Titanotheres, one or more of which gave The law cene the four phyla of Oligo- off collateral branches. Three of these phyla have now been shown to have a separate origin in the Middle Eocene. being sparsely represented by species of Weohipparion ( Gid- ley *) and a doubtful Pliohippus, the Camelidae by Pliau- chenia, the Dicotylide by several pieces of Platygonus, the Carnivora by an Amphicyon and other doubtful species of Canide. The “collateral lines of Camelide, so far as we know, died out, and the adaptive rediation of the true camels begins. However, no generalizations can as yet be made from this scanty fauna; we are confronted with more gaps in our knowledge and more unsolved problems than in any other period. Among these, the direct ancestry of the South American cameloids (Auchenia) as well as of the true camels (Camelus) should be found. We also should find here the stages directly ancestral to the horse ( Aquus), be- 2A New 1908, pp. 465-476. Three-toed Horse. Bull. Amer. Mus. Nat. Hist., vol. xix, Progress in Mammalian Palaeontology.—Osborn. 225 cause it now appears certain that Marsh’s Plzohippus was an Upper Miocene and not a Pliocene animal, and was, moreover, apparently on a side line not leading directly into Hquus (Gidley, Fig. 4). Thus not only is the Pliocene plains fauna sparsely known but the Pliocene forest fauna is wholly unknown. . Tue PuLeisroceNE Fauna. Equivalent to (1) the Preglacial, Forest Beds of Nor- folk (St. Prest. Durfort, Malbattu, Peyrolles), (2) Glacial, (Mid-Pleistocene, Lower Mid-Pleistocene), (3) Postglacial deposits of Northern Europe and Asia. Here again American paleontology is far behind that of Europe as to knowledge of the chronological succession of deposits, and a vast amount of work remains to be done in the discrimination of geological and faunal stages, in the comparison of Eastern and Western cave—and sand— de- posits, and in the coordination of the first appearance of man with that of the mammalian succession. The advent of the true Hywus marks the base of our Pleistocene, as shown in the sand deposits of the Western plains in the so-called Hguus beds. The geographical dis- © tribution and remarkable adaptive variation of the Pleisto- cene horses have now been fully worked out (Gidley’), prov- ing that there are ten species characteristic of different localities, and ranging in size from & giganteus larger than any modern horse, to the diminutive 2 monteZumae, But nowhere in North America have horses been found contem- poraneous with man. Two chief advances have been made, first, the distinc- tion of plains and river, from forest faunas; second, the exploration of two very remarkable cave deposits. The Western plains fauna of the Hguus beds or Lower Pleistocene (Matthew!) contains among the Carnivora, Canis, Dinocyon, Felis; among the Rodentia, Fiber, Arvi, cola, Cynomys, Thomomys, Castoroides; among the Eden- tata, Mylodon,; among the Perissodactyla, three species of 8 Tooth Characters and Revision of the Genus Equus. Bull. Amer. Mus. Nat. Hist., vol. iv, 1901, pp. 91-142. 1 List of Pleistocene Fanna from ‘ay Springs, Nebr. Bull. -Amer. Mus. Nat. Hist., yol. xvi, 1902, pp. 317-322. 226 The American Geologist. October, 1905 Equus; among the Artiodactyla, two species of the Dico- tylide; one species of the Camelidz, and two of the Antilo- capride ( Capromeryx, a new form, Matthew), and Antzlo- capra; among the Proboscidea, Hlephas columbi A similar plains fauna is that of Silver Lake, Oregon, which includes also two aquatic animals, Castor and Lutra. At Wash- tuckna Lake, Washington, is found a forest fauna which includes in addition to camels and horses, a badger, Zaaidea- three species of Felis, two of Alces, one of the American deer, Cariacus, and one of the goat Oreamnos ( Haploceros ) Our knowledge of the Western cave fauna has been enriched especially by the discoveries of Sinclair’ in Cali- fornia, in the Potter Creek Cave, probably of late Pleisto- cene age. This includes an extremely rich series chiefly of the mountain and forest type. Of fifty-two species, twenty- one are extinct, including a new member of the Ovine in the genus Huceratherium® (Sinclair ). With these animals are associated relics possibly of human origin. In the East, the Port Kennedy. Cave, also treated by Cope, has been ex- haustively investigated by Mercer’, and shown to contain fifty species of mammals, including chiefly forest types, among which are the Mastodon americanus, a tapir, and two species of Hguus. Again no human remains have been found. As regards phylogeny, the horses are evidently poly- phyletic ; but we have not as yet worked out the distinctign between possible representatives of the horses, asses, and zebras. The Proboscidea have been clearly distinguished (Pohlig, Lucas, Osborn’) into four great types Mastodon amercianus in the Eastern and Middle States; Hlephas prim- égenius in the North, practically identical with the north Asiatic Mammoth; Hlephas columbi chiefly in the Middle States but also in the Southern, and Hlephas imperator in the South and ranging north to the Middle States; these species represent profoundly different types both in skull 2 The Exploration of the Potter Creek Cave. Univ. Calif. Publ. Amer. Archaeol. & Ethn., vol. 2, No. 1, 1904. 3 Euceratherium. Univ. Calif. Publ. Bull. Dept. Geol., vol. 3, No. 20, 1904, pp. 411-418. 4 The Bone Cave at Port Kennedy. Jour. Acad. Nat. Sci. Phila., vol. Xi, spt 2.) 1899! 5 Evolution of the Proboscidea in North American. Science, N. §S., xvil, Feb. 18. 1908, p. 249. Progress in Mammalian Palaeontology.---Oshorn. 227 and tooth structure. Elephas columbi is analogous to the Elephas antiquus type of Europe; the lephas imperator is rather analogous to the /. meridionalis of Europe. It is altogether probable that these species evolved in Eurasia and arrived fully formed in America. Naturally their geo- graphical ranges overlap; but /. ¢mperator is never found in the extreme North, nor £ primigeniug in the extreme South. In conclusion, the great problem of all is the time of arrival of man amidst the Pleistocene fauna. This event is of such paramount importance that we must prepare for it by definitely determining the chronological stages of lower mammalian succession. At present man appears to be a late arrival, but personally I have a strong presentiment that hu- man remains will be found in an earlier Pleistocene stage than is generally supposed. CHIEF CENTRES OF ADAPTIVE RADIATION OF THE ORDERS OF MAMMALS. I—Jurassic Radiation (Partly Hypothetical). Monotremata (Hypothetical, i. e. fossil forms not yet rec- ognized.) Marsupialia (Triconodonta). Placentalia (Insectivora Primitiva, = Trituberculata.) II—Marsupial radiation, upper Cretaceous and Tertiary. Australia (chief centre), Antarctica and South America. Only one family (Didelphyidae) certainly known in North Amer- ica and Hurasia. IlI.—First or lower placental radiation, upper Cretaceous and lower Tertiary (= Meseutheria Osborn.) North America (chief centre), Eurove, Africa (Creodonta), probably extending also to South America. a. Orders Certainly Recognized. Creodonta, surviving to Lower Oligocene. Tillodontia, Middle Eccene (possibly related to Rodentia). Taeniodonta, probably related to Edentata Gravigrada. Condylarthra, surviving to Middle Eocene. Amblypeda, surviving to Upper Hocene. 228 The American Geologist. _ Onober ae b. Orders not certainly known in Basal Eocene but probably belonging to this radiation. Insectivera, giving rise to modern Insectivora. Lemuroidea. Rodentia, Not yet certainly known earlier than Middle Eocene. IV.—Second or Higher placental radiation (= Ceneutheria Osborn), A. Middle Eocene and Tertiary. Chief centres North America and Eurasia, migrating to Africa and South America. a. Orders derived trom first placental radiation. Edentata from Radiation III (North America only). Insectivora from Radiation J and III. Rodentia. b. Orders characteristic of second placental radiation. Cheiroptera. Carnivora (Fissipedia and Pinnipedia). Primates, Anthropoidea, possibly from Radiation III. Ferissodactyla, Lower Eocene. Artiodactyla, Middle Eocene. c. Centres of origin unknown. Nomarthra or Effodientia (Lower Oligocene of France, Necromanis Filhol.) Tubulidentata (First appearing in Lower Oligocene of France, Paleorycteropus Filho!). Chief centre Africa, migrating in upper Oligocene (Sirenia), lower Miocene (Proboscidea), and Pliocene (Hyracoidea) to Europe, to Asia (Hyracoidea). Also to North and South America (Proboscidea). : firenia, Middle and Upper Eocene. Proboscidea, Middle Eocene. Hyracoidea, Upper Eocene. Arsinoitherium. Barytherium. Chief centre South America. a. Autocthonous orders. Litopterna. Toxodontia. Typotheria. Astrapotheria. Pyrotheria. b. Autocthonous or derived orders, in part. Edentata, Suborders: Lorigata (Giyptodontia and Dasy- poda), Pilosa (Gravigrada, Tardigrada, Vermilingua). AMERICAN GEOLOGIST, VoL. XXXVI, PLaTE XII. AMEnICAN GroLouistT, VoL. XXXVI PuaTE XII. E — ee z U4 (7 St ple NORTH Line 9 7 RUtRvTo (J — Little Grow Schesk J Ny RA: < : LZ Yo{}) RATILESNAKE Bortes SHI eS ON A ES: J SY GEOLOGICAL MAP Il } St Francis Mission OF THE lal CENTRAL PART OF THE ROSEBUD INDIAN RESERVATION SOUTH DAKOTA. LouP TORK TERTIARY Mark L 2) % OLIGOCENE \é Mark O oe “5 ss N PS aed - \ ; : \ , E c A S K A eS ) UPPER SO = CRETACEOUS SG “ fe, sieve reieicrs | 2 | Wimnidetennmilmeds mares aaron act usin oy cress ote oreiet ote [icuaieve raises il From the area of the Iowan drift, post-lowan. | IST ATRESEON UNS Ne, 5: aroae ono Vays, Welaae BRE eeaiees iio a/ob a | oche alae 1 | | NAST OG OMS ERs e's orate tes asci be ahaciees otc erioiai aoe ks toenslicke il cop doshe eee 260 The American Geologist. October Ayes ea! > | 38 Be) seine AGE eeewiee 3% EBD o 3 On 5, A y AS fee °o From the area of the Wisconsin drift, post- | Wisconsin. Blephasy prin Semi Slee rue tre cits cle cise else lee | um [PReceh 5 <2 IDIOUTEH MM Siohiida doom. coudoosoaqeoowans Hag ollac oon co6 il WEAINIMOCI A ea cesis lea) cotencuoers ou tue Mer ereveeyccomtens | il 2 IMIASTOM OIE Bei< ccrcssoeeiere acetcrs cys ien eievensy enciecteiers 2 4 Wndeterminede mcs =e Wace a acinc oe sna a oS il | From alluvium, mostly sub-recent, but some, | perhaps, older. | | IDEA vebitlUUOTS! soso dos anosaccnoue. oaaallsacocaac Ar | 1M Meaheatoyol car een Neen Pen ecel aun Berka A baci Caat nicecu asl liearitay mie, rec | 2 | IMASTOCOM aa sqoeiectaey rote easton ert teieerertoh-teleep=t-fell fal neers 10 LWiniseneieaatuayeGl oy ycachs occa ols hho. Ole. chsouns-cen aiscietal ncio.e co-0 4 | Associated with these mastodon and mammoth fossils have been found also the bones of the buffalo, wolf, peccary deer and elk; also the “land shells Helicina, Succinea, Pryamidula, Bifidaria, Limnea and others which are characteristic of the loess.” “In Rock Island the loess which contained elephant bones also contained fragments of coniferous wood, and at Davenport, in Iowa, the peaty loess from which tusks and other bones were taken has a seam of diatomaceous earth, in which no less than thirty-three now living species of diatoms haye been identified.” The discovery of these land mammal fossils in the loess which contains the land shells so often egpealed to by those who adopt the wolian theory of the origin of the loess in the Mississippi val- ley, adds so much more of the same kind of evidence to the sup- port of that theory. It is only necessary to assume that the wind storms that buried the land shells in wind-blown dust and sand were, say, ten thousand times more violent and dust-laden than has been supposed, and that the great land animals that co- existed with the snails were overwhelmed at the same time. And, further, the winds must have been violent enough to rend apart their carcases and to seatter the bones of their skeletons for con- siderable distances asunder, even extracting the teeth from their sockets. It is a much more natural and simple matter to get the wind-blown dust and the laminated loess into superposition above these fossils than to get the fossils below considerable thicknesses of the laminated loess. The #olian hypothesis accomplishes this in a most admirable and satisfactory manner. From the foregoing table it is learned that the mastodon and the mammoth existed, perhaps, prior to the Kansan ice epoch, and continued into the Iowan epoch, into the Wisconsin and even into Review ot Recent Geological Literature. 261 the sub-recent, having become extinct perhaps not more than five thousand years ago. 5 As to man and the elephants, these data give no direct testi- mony that they were cotemporary, except in one instance. Mr. M. T. Myers, of Fort Madison, reports the finding of “one human leg bone and one flint arrow head” associated with the remains of the mammoth in the alluvium of Lee county, Iowa. This is in the region where so-called “elephant pipes” have been claimed to occur in mounds constructed by earlier inhabitants of the country. “At all events the evident recency of some of the proboscidean remains makes us expectant of some fortunate discovery giving conclusive proof that man lived on this continent while these huge mammals were yet here.” N. H wW. Indiana Department of Geology and Natural Resources. 29th Annual Report. W.S Buatcuiey, State Geologist, pp. 1-888; pl., 34; figs., 67; maps, 7; Indianapolis, 1905. In the introduction to this report Prof. Blatchley reviews the development of the natural resources of the state during the past ten years. During 1895 the total output of coal, oil, gas, building stone, clay-products and portland cement was $16,770,816, while in 1904 the total output of these same products was $36,028,755, or an increase of 115 per cent. The body of the book is made up of an article on “The Clays and Clay Industries of Indiana’ by W. S. Blatchley. In the open- ing chapter he treats of the technology of clay. The geological distribution of Indiana clays forms the subject of the second chap- ter which is followed by “The Clays of Indiana by Counties” in which the clays within five miles of transportation lines are taken up and discussed in detail. Analyses are given and suggestions made as to the possible utility of individual deposits. These are frequently accompanied by maps and halftones of the exposures. In the fourth chapter, the clay working industries of Indiana, he discusses the growth of the clay-working industries of the state from $3,858,350 in 1900, to $6,085,242 in 1904, and gives in detail the methods and processes of manufacture, tests and uses of the pro- ducts made from Indiana clays. These include paving material, sewer pipe and hollow wares, refractory products, pottery and allied products, dry pressed brick, structural terra cotta, building brick and tile and the production of clay for shipment. This article is calculated to be a practical aid to the development of the clay resources of the state and, while a larger number of maps would have added to its value, yet, it serves that end admirably. It is intended largely for the use of the layman and-is couched in the clear simple language characteristic of the author. The remaining quarter of the book contains five articles, the first of which is the report of the mine inspector, James Epperson. This shows the total output of coal for 1904 to be 9,872,404 tons against 9,992,553 tons for 1903. The next article is the report of 262 The American Geologist. October, Taye the gas inspector, Bryce A. Kinney, which is followed by a short. article by Prof. Blatchley on the utilization of convict labor in the making of road material. The petroleum industry of Indiana, by Blatechley, coneludes the geological part of the book. He states. that “The output for 1904 was greater than in any previous year, both in the number of barrels produced and in value, though the average market price declined nearly seven cents. Since 1898 each year has seen an increase in production, and in the seven years has. more than trebled.” The most important development during the year was in the Munsie-Parker-Selma field where a third “pay streak” was discovered 240 to 300 feet below the top of the Tren- ton rock at this place. The output for 1904 was 11,330,030 barrels valued at $12,127,107. The last article is by Melville T. Cook on the “Insect galls of Indiana.” J. W. B: MONTHLY AUTHOR'S CATALOGUE * OF AMERICAN GEOLOGICAL LITERATURE ARRANGED ALPHABETICALLY. ADAMS, F. D. The Monteregian hills; a Canadian petrographical province, (Can. Ree. Sci., vol. 9, p. 198, 1905). ADAMS, F. D. (and O. E. LE ROY). The Artesian and other deep wells on the island of Montreal. (Geol. Sur. Can., vol. 14, pp. 74, maps, 1904.) BABB, C. C. (See NEWELL, F. H.) BAIN, H. F. (See ECKEL, E..C.) HARRIS, G. D. A report on the establishment of tide gage work in Louisiana. Bull. 3, Geol. Sur. La., pp. 28, 1905. BASTIN, E. S. Note on Baked Clays and Natural Slags in eastern Yyoming. (Jour. Geol., vol. 13, pp. 408-418, July-Aug., 1905.) \ BERRY, E. W. The ancestors of the big trees. (Pop. Sci. Month., vol. 67, pp. 465-474, Sept., 1905.) BIBBINS, ARTHUR (See WARD, L. F.) BOUTWELL, J. M. (ARTHUR KEITH, S. F. EMMONS). Economic geology of the Bingham mining district, Utah. Prof. Pap. U. S. G. S., No. 38, pp. 410, pls. 49, 1905. Monthly Author's Catalogue. 263 MELLOR, E. T. ; Glacial (Dwyka) conglomerate of South Africa. (Am. Jour. Sci., vol. 20, pp. 107-119, Aug., 1905.) MURGOCI, G. M. Genesis of Riebeckite rocks. (Am. Jour. Sci., vol. 20, pp. 33- 146, Aug., 1905.) NEWELL, F. H. (and R. E. HORTON, N. C. GROVER, J. C. HOYT.) Report of the Progress of Stream Measurements for the year 1904. U.S. G.S. Wat. Sup. & Irr. Pap. No. 125, pp. 114, pls. 2, 1905. NEWELL, F. H. (and C. C. BABB, and J. C. HOYT). Report of Progress of Stream Measurements for the Calendar Year 1904. U.S. G. S. Wat. Sup. and Irr. Pap. No. 130, pp. 204, pls. 2, 1905. NEWELL, F. H. (D. W. ROSS, J. T. WHISTLER, T. A. NOBLE). Report of progress of stream measurements for the calendar year 1904. Wat. Sup. & Irr. Pap. No. 135, pp. 300, 1905. NOBLE, T. A. (See NEWELL, F. H.) OSBORN, H. F. Western explorations for fossil vertebrates. (Pop. Sci. Month., vol. 67, p. 561, Oct., 1905.) OSBORN, H. F. Skull and skeleton of sauropodous dinosaurs Morasaurus and Brontosaurus. (Science, vol. 22, p. 374, Sept. 22, 1905.) Vea Rea OSBORN, H. F. Recent vertebrate paleontology. (Science, vol. 22, p. 18, Aug. 11, 1905.) PECK, F. B. The tale deposits of Phillipsburg, N. J., and Easton, Pa. (An. Rep. State Geologist, N. J., 1904, pp. 163-185.) BIO a PENFIELD, S. L. (and G. S. JAMIESON). Tychite, a new mineral from Borax lake, California, and on its artificial production and on its relations to northrupite. (Am. Jour. Sci., vol. 20, pp. 217-225, Sept., 1905.) PERKINS, W. R. (See LOGAN, W. N.) PRATHER, J. K. The Atlantic Highland Section of the New Jersey Cretacic. (Am. Geol., vol. 36, pp. 162-179, Sept., 1905.) PRINDLE, L. M. The gold placens of the Fortymile, Birch Creek and Fairbanks regions, Alaska. Bull. 261, U. S. Geol. Sur., pp. 84, pls. 16, 1905. PROSSER, CHAS. S. The Delaware Limestone. (Jour. Geol., vol. 18, pp. 413-443, July-Aug., 1905.) 264 The American Geologist. October, 1905 PROSSER, CHAS. S. Notes on the Permian Formation of Kansas. (Am. Geol., vol. 13, pp. 143-162, Sept., 1905.) 1 RAFTER, GEO. W. Hydrolology of the State of New York. New York State Mus. Bull. 85, pp. 902, pls. 45, maps 5, 1905. : REID, J. A. The structure and genesis of the Comstock lode. (Univ. Cal., Bull. Geol. Dept., vol. 4, pp. 177-199.) RIES, H. : The production of flint and feldspar in 1904. (Min. Rese. U. Ship U. S. Geol. Sur. 1904, 5 pp.) ROSS, D. W. (See NEWALL, F. H.) SLICHTER, CHAS. S. Observations on the Ground Watens of Rio Grande Valley. U. Ss. G. S. Wat. Sup. and Irr. Pap. No. 141, pp. 81, pls. 5, 1905. SPURR, J. EDW. Descriptive Geology of Nevada South of the Fortieth Parallel and Adjacent Portions of California (Second Edition) U. S. G. S. Bull. No. 208, pp. 229, pls. 8, map, 1905. STANTON, T. W. Stratigraphic notes on Malone mountain and the surrounding region near Sierra Blanca, Tex. (Bull. U. S. G. S., No. 266, pp. 23-33, 1905.) \ STONE, R. W. Mineral Resources of the Elders range quadrangle, Pennsyl- vania. U. S. G. S., Bull. No. 256, pp. 1905. TAFF, J. A. : Description of the Tahlequak folio. U. S. Geol. Sur., Geol. Atlas; Folio No. 122, 1905. WARD, L. F. (W. M. FONTAINE, ARTHUR BIBBINS, G. R. WIE- LAND). : Status of the Mesozoic flora in the United States, second paper. Part I, text, and Part 2, plates. Mon. U. S. Geol. Sur., vol. 48, pp. 616, pls. 119, 1905. WARING, G. A. Quartz from San Diego county, California. (Am. Jour. Sci., vol. 20, pp. 125-128, Aug., 1905.) WEEKS, F. B: Bibliography and index of North American Geology, Paleontol- ogy, Petrology and Mineralogy, for the year 1904. U.S. Geol. Sur., Bull. 2745" pp! 218; 1905: WHISTLER, J. T. (See NEWELL, F. H.) Correspondence. 265 WIELAND, G. R. (See WARD, L. F.) WOODWORTH, J. B. 2 Pleistocene Geology of Mooers Quadrangle, New York State Mus., Bull. 83, pp. 60, pls. 25, map, 1905. WOODWORTH, J. B. Ancient water-levels of the Champlain and Hudson valleys, N. Y. State Mus@um, Bull. 84, pp. 265, plates 28, July, 1905. CORRESPONDENCE Economic GEOLOGY IN PERU.—It might be of some interest to the readers of the AmeErRIcAN GeEoLoaist to learn something about the scientific organization recently created by the government of Peru to investigate the natural resources of the republic. Owing to the very rapid development of the various mining industries, the establishment of a bureau which should be authorized by the gov- ernment to locate and fix boundaries of mining claims, collect sta- tistics relative to the production and values of ores, and accumu- late various data relative to the geology, mineralogy, and geog- raphy of the country, became an immediate necessity. Accordingly in 1902 the bureau now known as the “Cuerpo de Ingenieros de Minas del Peru” was established with Sr. J. Balta, the present min- ister of public works, as the director. It was soon discovered how- ever, that the subjects and projects demanding the immediate and serious consideration of this organization were so numerous and varied in kind, that it became highly advisable to classify the work in hand and distribute allied lines of investigation to independent commissions each with its chief and corp of assistants, the series of commissions, however, being under the general charge of the Director of the “Cuerpo,” Sr. Marco A. Denegeri. The divisions of the “Cuerpo” are as follows: 1. Division of Mines, established 1902, including: (a) Permanent commissions in large mining areas, to locate claims, fix boundaries, etc. (b) Exploratory commissions to investigate and report upon newly discovered mining areas. 2. Division of Water Supply, established 1904, including: (a) Engineering projects relating to the storage and distribu- tion of surface water for irrigation purposes. (b) Geological Investigations to determine oe and distribu- tion of underground waters. 3. Division of Economic Geology, established in 1904. 266 The American Geologist. October, 1905 All these commissions have their responsible chiefs and one or more assistants and among these chiefs are four American special- ists, namely, Dr. George T. Adams, in charge of underground waters, M. H. Hurd and Chas. W. Sutton for engineering and topographic work, and Mr. V. F. Marsters for economic geology. The only non- Peruvian technical assistant is Mr. H. T. Stiles, who is under the direction of Mr. Hurd. At this time there are at work: 2 Permanent mining commissions. 6 Exploratory mining commissions. 1 Economie geology commission. 2 Topographie and water-supply commissions. 1 Underground water commission. Generally the names of the permanent commissions are taken from the districts in which they are located, e. g., the Cerro de Pasco, Yauli Ica, Callao, ete. commissions. Each commission is al lowed a certain sum of money which is under the direct control of the responsible chief. The object of the geological commission is to investigate specific problems relative to the development of the metallic and non metallic deposits of Peru. This department constitutes the first official geological survey in the republic. The first problem to be considered will be the geology of the oil fields of northern Peru (Provinee of Tumbes.) While the “Cuerpo” has been in existence but a little over three years some twenty-six bulletins dealing with a wide range of subjects have been published. These may be obtained by appli- cation to the Director, Sr. Denegeri. Lima, Peru, Sept. 12, 1905. V. F Marsters MaTEO TEPEE —A little over a year ago, while going over sev- eral new works, the writer was struck by the many ways in which the several authors had in spelling the same words. Several in- stances were noted, but one of the best illustrations was that of a voleanic tower in the northeastern corner of Wyoming—‘“Mateo Tepee,” or what is more popularly known as the “Devil’s Tower.” This tower of perpendicular basaltic columns, may be seen to the right of the Burlington railroad in going west, between New Cas- tle and Sheridan, Wyoming. According to Newton and Jenney, it has an elevation of 625 feet from the surrounding country and may be seen for many miles around. Professors Chamberlin and Salisbury spell it in their new Geol- ogy, page 156, fig. 124, “Matteo Tepee,” locality Wyoming. Prof. R. S. Tarr, spells it, in his “New Physical Geograrhy,” fig 231, facing page 127, “Mato Tepee” locality Wyoming. In the May number 1904, of the American GEOLOGIST, under the title of “Hditorial Comment, Peleliths,’ plate 22 facing page 324, the same name is spelled “Mato Teepee” and the locality given as South Dakota. In the “Report on the Geology and Resources of the Black Hills Personal and Scientific News. 267 of Dakota” by Henry Newton and Walter P. Jenney, 1875, published 1889, it is spelled again Mato Teepee and the locality given as Dakota—i. e. one would infer as much from the title of the report. However, a map of the Black Hills was prepared by these gentle- men and accompanies the report, and shows the tower to be in Wyoming. At the time this report was made the tower was called “The Bad God’s Tower” or in other words ‘The Devil's Tower.” The boundary line between South Dakota and Wyoming is a little west of 104° or about 104°-1’-20”. ‘Mateo Tepee” or “Bear Lodge” as Newton and Jenney called it, is located on their map ’ at almost exactly 104° 45’ W. Long. and 44° 35’ N. Latitude. This -places it in the northeast corner of Wyoming, in Crook county. The name, ‘Mateo Tepee,” is of course of Indian origin, prob- ably from the Sioux, and literally means “Bear Wigwam”—Mateo, pronounced Mah-to—meaning bear and “ Tepee’’ meaning wigwam, lodge, or a conical tent. In former days this region (around the Devil’s Tower) was a g reat bear country and was visited each year by the Indian bear hunters—hence the name. In conclusion the writer believes this name should be spelled “Mateo Tepee” and the locality is without a doubt in Wyoming. J P Rowe University of Montana, Missoula, September 21, 1905. PERSONAL AND SCIENTIFIC NEWS. ILLINOIS GEOLOGICAL SuRVEY. At the last session of the legislature a bill was passed establishing a geological sur- vey of the state and making an appropriation of $25,000 per year for this purpose. Of this amount $10,000 may, at the discretion of the board of control, be used for topographic mapping in cooperation with the U. S. Geological Survey. This cooperative work has been undertaken for the present year, at least, and work along this line was begun about the first of June. The board of control consists of the governor of the state, the president of the State University and one other member to be appointed by the governor. Gov. Deneen this summer appointed as the third member of the board JPror. -t. Cye-Chamberlin. , The headquarters. of: the survey are to be at the State University at Champaign and the University furnishes rooms for the survey. For print- ing, etc. $5,000 is available from the state printing funds. Dr. H. Foster Bain, of the U. S. Geological Survey has ac- cepted the position of state geologist and enters upon this work November Ist. 268 The American Geologist. October, 1905” University oF Wisconsin. During the coming Janu- ary Mr. Bailey Willis, of the United States Geological Sur- vey and Carnegie Institution, will present a course of twelve lectures in the Geological Department of the University of Wisconsin on the subject of “Continental variations, with special reference to North America.” The course is given primarily for students making geology a major study, and is open to such students not regularly registered at this university. IN THE YEAR 1904 THERE WERE OBSERVED in Norway 35 earthquakes, of which the most severe was on the 23rd of October, and more than half of the whole number occurred after that date-—Kolderup. Dr. US. GRANT RETURNED from Alaska, passing through Minneapolis in the early part of September, in time to resume his work at Northwestern University. DR. W, J. McGEE HAS BEEN APPOINTED DIRECTOR Of the Public Museum at St. Louis. THE LakE SupERIoR MininG Institute will hold its eleventh annual meeting on the Menominee range at Ish- peming, Mich., October 17, 18 and 19. There will be trips by: train to Crystal Falls, Iron; Mountain, Escanaba and Gladstone. Pror. CHARLES SCHUCHERT of Yale University, has returned from a geological trip extending over the ancient formations of Nova Scotia, New Brunswick and eastern Quebec. E. H. SELiarps late of the University of Kansas, is in charge of the departments of zoology and geology at the University of the state of Florida. W. J. MILLER HAS BEEN APPOINTED to succeed professor C. H. Smyth Jr, in geology, at Hamilton college, and M. W. Twitchell has been appointed to the chair of geology at South Carolina college, Columbia, S. C. Pror. C. N. Goutp of the University of Oklahoma, will be absent the current college year and his duties will be discharged by Prof. E. G. Woodruff. CuarLEs W. Brown has been appointed instructor in geology and mineralogy at Brown University. THE AMERICAN GEOLOGIST. VOL. XXXVI. PLATE XIV Quarry in a Glacially Transported Mass of Chalk, near Malmé, in South- ern Sweden. {Photograph by Dr. N. O. Holst. | THE Pore aAN GEOEOGIST. VOL. XXXVI, NOVEMBER, 10s. No. 5. GLACIAL MOVEMENTS IN SOUTHERN SWEDEN. By Pror. G. FREDERICK WRIGHT, Oberlin, Ohio, PLATE XIV. Having had the privilege of spending two or three days with Dr. N. O. Holst, while he was engaged in surveying for the geological map of Skane, the southern province of Sweden, I am permitted to bring before the English public some of the important and remarkable discoveries which he has made. These relate first to the direction and force of the ice movement, and secondly to the unity of the period. Skane, the most fertile province of Sweden, projects southward of the main peninsula so as to make it almost a part of Denmark, to which by virtue of its physical geo- graphy it properly belongs. It is completely covered with glacial deposits to a depth of 100 or 200 feet. A very well defined terminal moraine runs across the province east and west, about midway between the north and south boun- daries. The material in this moraine is to a considerable extent derived from Finland, showing that the center of glacial dispersion was somewhat farther east in Scandinavia than has been supposed. Both the direction of the moraine and the material of which it is constituted’ show that in southern Skane the final ice movement had a northwesterly direction. That is, the ice, after moving down the axis of the Baltic sea in a southwesterly direction, when it passed the low mountains bordering the northeastern part of Skane, must have found the line of least resistance in the direction of the North sea, causing it to turn around towards the north, 270 The American Geologist. November, 1905 as the lake Erie ice is known to have done in southern Michigan and northern Indiana. The most striking indication of this is found in the position of an immense mass of chalk which is included in the moraine about five miles east of Malmo. This chalk mass extends three miles in a_ northeast and southwest direction, averages 1,000 feet in width, and from 100 to 200 feet in thickness, being, so far as I know, the largest boulder, or glacially transported mass, that has been described. It is everywhere covered with till, and almost everywhere has till underneath it. Its regular position is between what we should call the upper and the lower till, the upper till being yellow and the lower blue. But in one place, which I ex- amined, the lower or blue till was both above and below it. While the chalk is together in one mass, it everywhere shows signs of immense pressure and disturbance, being broken up into small cubes, and having its flint nodules cracked and arranged in lines simulating stratification. The upper part of the chalk has also been extensively sheared off and mingled with the till. This mass of chalk has been brought fully to light through its commercial value, eight or ten companies having mined or quarried it for many years. It belongs to the true soft chalk of Cretaceous age, and was supposed by the earlier geologists to indicate a Cretaceous area, where it was least to be expected, since the chalk which mainly under- lies the peninsula belongs to the Trias or Lias. The de- termination of its glacial transportation has therefore solved a very difficult problem. It must have been picked up bodily from the shores or bed of the Baltic sea, being trans- ferred westward many miles to its present position. Dr. Holst is bringing to light much mew evidence bearing upon the unity of the Glacial period, and is more than ever confirmed in his adhesion to the theory that the upper till and the lower till are of the same age,—the lower till being that which was dragg-d along under the ice, and the upper till the material which was incorporated in the ice, and which so became oxidized in the process of trans- mission and deposition. In many cases which-he showed me, this would certainly appear to be the fact, as indicated Glacial Movements in Sweden. — Wright. 271 by the sharp line which separates the blue from the yellow till. , But the most important discoveries bearing upon this point were found at Tapplelargo, twelve miles east from Malmo. Here is an area of several acres covered with an overwash deposit from the moraine, which is a mile or more to the south. Ina stratum of clay, about seven feet thick, many species of shells and plants are found, indicating peculiar conditions which can be accounted for only by sup- posing that during the final melting away of the ice the summers became very warm, so as_ to allow temperate species to flourish close up to the ice-front, thus allowing them to mingle with arctic or subarctic species. It is evident from inspection of the stratum that these species lived and were deposited contemporaneously, and not by an advance of the ice after an interglacial period. This would seem to meet the case of comingling of tem- perate and subarctic species which Coleman has described in the vicinity of Toronto, and so it will greatly simplify our interpretation of glacial phenomena in the northern United States and Canada. BOLSON PLAINS OF THE SOUTHWEST. By W. G. TicHT, Albuquerque, N. M. There seems to be a very decided tendency on the part of students in physiographic geology to enlarge upon the conceptions of topographic types, as they are originally described, and in the subsequent study of the topographic features of any particular section, to describe those features in terms of the modified conception of the type forms. As a result there develops a very confused idea in the minds of workers concerning the true type, and with that misconception in mind the correct interpretation of any par- ticular region becomes doubtful, and the description of that region almost wholly unintelligible, giving to the student who has access to the literature alone, a radical misconcep; tion of the true topographic conditions. As an example of my meaning the term “peneplain” may be taken. It would be interesting to know how many times 272 The American Geologist. Hoyenibes ae an aggradation plain of some sort has been mistaken for a degradation plain and called a peneplain. There are un- doubtedly many cases where the two types of plains look nearly alike and only a careful study would determine the true character. This superficial resemblance, which extends to various types of topographic forms, is a constant source of error. The most serious mistakes are made when two types of radically different origin and structure are classed together and made the basis for broad generalizations. When an author has described a certain type of topo- graphic form, presumably from a careful study of some definite region, and has given a name to that type, it can only lead to much confusion and error when the same name is used by another to describe a different form, or to attempt to modify the meaning of the term to fit other conditions. It is not intended at the present writing to discuss the uses and abuses of he term “bolson” as applied to inter- montane valleys but rather to take the term as originally described* and apply it to the study of the great valleys of the southwest and especially to New Mexico. To quote briefly: “Bolsons are generally floored with loose, unconsolidated sediments derived from the higher peripheral regions. Along the margins of these plains are talus hills and fans of boulders, and other wash-deposits -brought down by mountain freshets. The sediments of some of the bolsons may be of lacustral origin.” “The bolson plains on the other hand,” (as distinguished from plateau plains) “are newer and later topographic fedtures, consisting of structural valleys between mountains or plateau plains, which have been partially filled with debris derived from the adjacent eminences.” “The bolson plains are constructional detritus plains filling old structure troughs.” It seems that this description is clear enough. The type form is not dependent upon the characters of the bordering mountains nor the character or structure of the deeper valley floor, nor is it especially concerned with the total thickness of the wash-deposits over the floor of the *HILL, Top. Atlas, U. S., folio 5, p. 8, 1900: Bolson Plains of the Southwest—Tight., 273 older valley, except in so far as these deposits must con- tribute an important factor in determining the character- istics of the topography. An important element in this definition depends upon the interpretation of the word “plain.” A bolson is genetically related to other construc- tural plains, such as flood plains and terrace plains of river valleys. In the flood plain and terrace plain deposits the plains are more or less narrow and parallel with the stream, which furnishes the major portion of the deposits. On the other hand in the bolson, while the deposits are of fluviatile origin (or largely so) the plain loses the characters of a flood plain or terrace plain in that it is generally much broader and the material “is derived from adjacent emin- ences,” and the plain is of such an extent that the “talus hills and fan cones and wash-deposits brought down by the mountain freshets” form only the bordering characters of the plain, but point unmistakably to the origin of much of the deposits forming the floor of the bolson. If we look for a moment at the forces involved in the formation of a bolson we see that there must exist an ex- tensive trough in which the contribution of material from the sides of the bordering mountains is much greater than the capacity of the pre-existing drainage to remove, or that in the structural formation of the valley there is formed a closed basin and into this the lateral materials are de- posited. In the closed basin type, the basin may or may not be the location of a lake. If the older trough has free drainage to start with the lateral introduction of debris may be such as to divide an otherwise continuous stream course into a series of lake basins or to even totally obliter- ate the through-flowing stream as a surface feature. Mr. Hill says: “These plains or ‘basins’ as they are sometimes called are largely structural in origin,” and again he uses the terms “structural valleys between moun- tains and plateau plains.” If it were intended to confine the term bolson to those forms which occur in strictly structural valleys which have ‘not beet subseqitently modi- fied by erosion; it would’ have a very limitéd'use indeed, for but few valleys of that type are to be found, and the author’s iHtastrations db ‘not indicate’ this' limited tse.’ Buf I'take it 274 The American Geologist. Neverien a that the term “structural valley” or “structural trough” was used in reference to the large features of the topography as distinguished from simply valleys of erosion cut mainly by stream action. The very essential feature of a bolson is that the plain is bordered by mountain forms or plateau escarpments. The mountains may be of the fold or fault type, but rising as they do above the general level’of the plateau upon which they stand the intervening area might properly be considered a structural valley. In some cases this intervening area may be so protected from erosion by the distribution of the mountain uplifts that it will be pre- served and will present the structural characters of the original plateau plains. Again it may be in the line of the great longitudinal drainage lines of the plateau and be large- ly removed by subsequent erosion. As far as_ the later formation of a bolson is concerned, it would appear that either type might properly be called a structural valley, and with the later deposition of the detritus forming the bolson plain, there would be a striking difference in the thickness of the deposits, those in the eroded structural valley being much thicker. It would appear also that in the formation of such a structural valley by the enclosure of a portion of a plateau by the elevation of bordering mountains, where the vallev is not subjected to subsequent erosion and the remaining valley floor is fairly horizontal, there would be produced a topographic form which would resemble very closely the bolson but which would be as essentially different from it as an aggradation plain is different from a _ peneplain. These two forms having similar superficial characters may be easily mistaken, the one for the other, for with the eleva- tion of the bordering mountains enclosing a structural valley free from erosion, there will most certainly develop around the margin of the remnant of the enclosed plateau plain, talus hills and fan cones and frontal wash aprons which will rapidly work out over the floor of the valley and eventually convert it into a bolson plain while the superficial charac- teristics may remain almost the same during the entire pro- cess. : It is apparent that wher the filling of the valley takes Bolson Plains of the Southwest—Tight. 275 place over the floor of the great structural valley, the pro- duction of the bolson does not materially modify the topo- graphic features, but when the great structural valley has been deeply eroded and then subsequently filled the produc- tion of the bolson does make a decided difference in the topographic relations of valley and mountains. We see then, that the bolson plain finds its proper place in the series of constructional plains derived from fluviatile actions, and the lowest member of the series is represented by the flood plain of the river, in which the material is almost wholly derived from the longitudinal action of the stream; while the bolson plains are at the opposite end of the series, in which the longitudinal stream may contribute largely in some stages of the building of the plain but that the pre- dominant factor is the derivation of material from the bor- dering hights by torrential action of temporary streams and rivulets which are produced largely by rainfall. This in general is the writer’s understanding of the use of the term bolson, as applied to many of the great inter- montane plains of the southwestern plateau and great basin region. Whether the writer is correct or not in his inter- pretation of the use of this term, it is certain that under any definition of the term there is found in this region a large number of valley plains having very diverse characters and very diverse origins. The writer cannot therefore agree with Dr. Chas. R. Keyes of Socorro, in his discussion of the bolson plains of New Mexico in the AMERICAN GEOLOGIST for September, 1904. Dr. Keyes has grouped under this term such plains as the Jornada del Muerto, San Augustine, Estancia, Mimbers and. the great plains along the Rio Grande, Rio Pecos and-Canadian rivers. He has seemed to correlate these plains, with others, with the great Llano Estacada of Texas and other great plains to the southwest. If Dr. Keyes’ correlations are correct, it does not seem to the writer that these great intermontane plains of the New Mexico region can be by any definition classed as bolson plains and many of them certainly conform to that defini- tion. In view of this difference of opinion it seems advisa- ble to call attention to some of the features of some of these various plains in detail. It is well understood that the 276 The American Geologist. Noveniber, 1905 great stake plains of Texas are made up largely of Creta- ceous sediments which have a more or less regular dip from the frontal ranges of the Rocky mountains to the gulf of Mexico. Toward the New Mexico border of this plain the strata have stronger dip and erosion has exposed the edges of the strata along the Rocky mountain front. The Creta- ceous terranes are covered with a mantle of Tertiary gravels derived from the mountain front. Dr. Keyes says: “The Las Vegas plateau, Llano Esta- cada, the bolson plains of New Mexico, and some of the broken plains of eastern Arizona seem to belong genetically together ;” and he further says: “When the general bow- ing up of the region took place in Tertiary times, the great plain formed was partly a pleneplain of destructional land origin and partly a constructional plain of marine origin.” From this it would appear that the bolson plains of New Mexico, as he describes them, are remnants of this old peneplain, and that the mountain blocks of the plateau of New Mexico were formed subsequent to the peneplanation of the Cretaceous and lateral beds. It is not possible at the present writing to present the data to show that the struc- ture of the mountains of New Mexico will not sustain this position. It is the writer’s desire in this discussion, to con- fine attention wholly to the valley forms. Dr. Keyes says: ‘That the old bolson plain in the Rio Grande valley is at present about 1,500 feet above the river’ and he refers to the Colorado river as being “a mile deep in its canyon” below the surface of the great plain which he has constructed in his hypothesis. During a residence of four years in the Rio Grande valley, accompanied with considerable field work, it has not been my pleasure to see a single remnant of the old plain to which reference is made. The valley of the Rio Grande through New Mexico has an extremely complex and varied form, and history. I desire at the present writing to call attention to only a few points in its history bearing upon the particular discussion in hand, and ‘what is’ said with reference to the valley includes only that section which lies within the territory of New Mexico, ' The river is at several points, notably at’ Whité Rock canyon, at Eléphant buttes, - Bolson Plains of the Southwest.—Tight. 277 and at El Paso, cutting through a rock gorge upon a rock floor, but throughout most of its course it is meandering over a broad flood plain in a still broader shallow trough, the latter cut some 200 or 300 feet below the surface of the broad sheet of plain deposits locally known as mesas. The larger structural valley which is followed by the Rio Grande is undoubtedly of very complex origin and no gen- eral description would be adequate for any particular sec- tion of the river. From the limited amount of data in hand it would appear that in some sections the river is following the line of a great fault zone and in other sections it is apparently following along the axis of an immense anticline, which has been very deeply and broadly eroded. The great structural valley presents an average width of fifteen to twenty miles, measured across the surface of the great mesa plain. ; If we examine into the structure of the mesas border- ing the river, as presented by well sections and deeply cut atroyos, we find that it is made up wholly of sands, gravels, and clays of fluviatile origin. The materials composing the mesas have been largely derived from the lateral mountains. The depth of this mesa deposit in the old structural valley is not definitely known. A well over seven hundred feet deep at Albuquerque did not reveal the rock and as the top of this well is about 250 feet below the surface of the mesa plain and near the central portion of the great valley, we can see that the great structural trough has been filled by the mesa deposits to the depth of probably much more than a thousand feet. It is evident from many topographic features that the river once meandered over the upper sur- face of this mesa plain at least 250 feet above its present level. At about that time in the history of New Mexico there occurred a more or less general extrusion of basaltic lavas over many areas. At least two of these lava overflows reached down into the valley of the Rio Grande and attained such magnitude ‘as to ‘produce ' profound changes ih the course of the river.’ The first of these which I will mention is the great lava flow in northern New Mexico which dam- med the coursée of the Rio Grande ‘above the White Rock canyon, and the second, the great lava’ flow south of San 278 The American Geologist. November, Dane Marcial, which deflected the course of the Rio Grande far to the west of its old valley through the Elephant Butte canyon and west of the Sierra de los Caballos, reaching its old course again just a little north of Las Cruces. -The Jornada del Muerto lying between the San Andreas and the Sierra de los Caballos is undoubtedly the old valley of the Rio Grande, from which the river was diverted at the time of maximum aggradation and at the time of the great San Marcial lava flow. There is every reason to believe, from a careful study of the history of the Rio Grande that a cross section at the Jornada del Muerto is comparable in its history to a cross section of the river at Albuquerque, where the mesa deposits are known to be at least a thousand feet in depth. It is therefore evident that the plain of Jornada is in no way genetically related to the Llano Estacado, ex- cept in so far as concerns the Tertiary deposits of the latter. That the great mesas bordering the Rio Grande are wholly of fluviatile origin is further shown from the topographic characteristics in the vicinity of El] Paso where the river runs through a narrow rock channel between the Franklin mountains and the range to the southwest. Some few miles above El Paso, and on the west of the Franklin mountains are preserved other extensive remnants of the old gravel and talus plains which extend out from the canyons of the Franklin mountains at a level of 300 or 400 feet above the Rio Grande. Several miles to the west across the immediate channel of the Rio Grande are seen the opposite exposures of the same beds. Whether it was by the blocking of the old channel with another lava flow farther to the west or by the normal process of excessive aggradation, that the Rio Grande was forced through the narrow mountain pass at El Paso is yet undetermined, but that it is superposed in its present position upon an ancient col at El Paso is certain. The second instance to which attention is directed is the great basin in New Mexico lying between the San An- dreas and the Sacramento mountains, known as the White sands plain or the Hueco bolson.* This certainly is a typical bolson as the writer understands the use of the term. These * Hinz, U. S. Folio, No. 3, p: 9. Bolson Plains of the Southwest.— Tight. 279 great plains are some sixty or seventy miles long and twen- ty to thirty miles wide with the Sacramento mountains on the east rising to an average level of 6,000 or 7,000 feet above the plains and the San Andreas and Organs on the west and the Sierra Oscuras on the north rising to a some- what less elevation. The plains are very level or slightly depressed through the central axis and show a decided grade toward the south. In the upper part of this great plains valley are the white sands and the salt marshes of the ancient lake Otero basin recently described by Prof. C. L. Herrick, late of Socorro, New Mexico, in the September number of the GEoLocist 1904. At the northern end of the plains lies one of the most extensive lava flows in New Mexico, surpassed only probably by the great northern lava flow in Ria Arriba and ‘Taos counties, and in western Valencia county. That the deposits forming the floor of this great basin are very deep and composed almost entirely of fluviatile material has been demonstrated by numerous wells which have been sunk through various portions of the plain ranging in depth from a few feet to a well in the southern portion of the plain over 2,000 feet deep, which did not even at that extreme depth reveal the rock. North of the great lava, flow lies the Chapedero mesa and still farther north of that are the Estancia plains (San- doval bolson of Hill). While it cannot be definitely assert- ed with the data in hand, there are many facts which would seem to indicate that the Estancia plains and the white sands plains represent a g reat north and south structural valley, more or less parallel to the Rio Grande valley, from which the ancient river which occupied it, was either diverted by the extensive lava flows or by the normal pro- cesses of aggradation, or, what also seems very probable, that the sediments of the great bolson plains in these great structural valley sections have reached such enormous thickness that the waters of the through flowing drainage are at present entirely subterranean. There are many facts in hand to prove that there is a subterranean drainage which passes out of the southern end of this great axial trough. In refetring to the region of the Rio Pecos, Dr. Keyes says: “Of these the last two streams mentioned” (Rio 280 The American Geologist. evenber Auue Pecos and Rio Grande) “flow in the broad valleys between lines of block mountains,” And in another place refers to the long basin plains of the Pecos and states that the Pecos has cut down to a depth of 2,500 feet below the level of the’ old plain. It would seem that Dr. Keyes has failed to rec- ognize the fact that the Rio Pecos derives most of its water supply from the eastern side of the ranges of the Rocky mountains ; that the drainage of the river corresponds very closely with the strike of the Cretaceous beds, the Pecos itself being a very asymmetric river, having all of its tribu- taries of any consequence on its western side. And when it is borne in mind that the river is flowing in its southern course through southeastern New Mexico along the out- crop of a great bed of gypsum and that the Cretaceous ter- ranes of the Llano Estacado are dipping to the eastward it will be seen that in the development of the Pecos valley the axial stream has been migrating slowly eastward down the ‘dip of the strata against the edge of a hard stratum. On the westetrn side of the Pecos the surface of the region con- forms very closely with a very hard limestone element of the Cretaceous series which rises rapidly toward the west nearly to the crests of the bordering mountains, while on the eastern side of the river there is a sharp escarpment of a few hundred feet from the upper edge of which extends the great plain of the Llano Estacado, which slopes gradually to the southeast, the surface of which is strewn with the ‘Tertiary gravels. The Rio Pecos, therefore has no moun- tains bordering the eastern side of its valley and there are no extensive detrital plains in any way comparable to those of the Rio Grande along the course of the Pecos outside of the mountain valleys at its head waters, except the great frontal apron of Tertiary mountain wash just referred to. If we are to assume that two thousand feet of sedi- ments have been removed from the Llano Estacado then it might be proper to say that the Pecos is flowing 2,500 feet below the aggradation surface of the Cretaceous terranes; otherwise we must consider that the major portion of the valley of the Pecos is-scarcely more than a good sized drain- age ditch along the line of strike of the hard beds of the Cretaceous formatiom which’ underliés the Staked Plains region. Bolson Plains of the Southwest.—Tight. 281 Concerning the bolsons of the Rio Mimbres or Ante- lope plains I have little data at hand except that it is well known that underneath the Antelope plains there is a large supply of subterranean water contained in deeply buried river gravels. It has never been my pleasure to visit the San Augustine plains, therefore | cannot speak authorita- tively concerning this extensive bolson. With this brief statement concerning some of the physi- ographic and structural features of New Mexico it seems to the writer that Dr. Keyes is not justified in classifying as a common physiographic type the great plains of the Llano Estacado to the eastward of New Mexico and the typical dolsons which occur within its borders. In the judgment of the writer it would not even be possible to place the border plains of the Rio Grande and of the Rio Pecos in the class of bolsons, and certainly such plains as the Hueco, Minibres, the Estancia and the Jornado can bear no relation whatever to the. great plateau plain through which the Colorado river has cut its grand canyon. From the data in hand it appears to the writer that in New Mexico and much of the great basins region where the colson plains form an important physiographic type, there is a common history of origin. The whole region has been ai some time at a very much higher level than at present and subjected to such erosion that the great structural val- luis of the entire region were worn out several thousand feet in depth. Every feature of origin seems to point with unmistakable finger to a time of such erosion, under atmos- pheric conditions of heavy participation, with a much higher elevation of the plateau than at the present time. There certainly was a time when the carrying capacity of the axial streams of all the valleys was much in excess of the loads of material furnished to them by their lateral tributaries and by torrential action of the characteristic method of precipi- tation of the semi-arid region, resulting in the supply of en- ormous quantities of material from the steep mountain slopes into the valleys in such quantities that the larger streams were vastly overtaxed and the period of aggradation was inaugurated. This period continued until the deposit in these ancient valleys accumulated to thousands of feet 282 The American Geologist. November, 1908 in thickness. In many cases the valleys were so completely filled that the detrital plains of the neighboring valleys were united, giving the appearance of extensive plains with iso- lated islands or bordering ridges. Where the flow of water in the larger drainage axis like the Rio Grande was sufficient, the river contributed largely in the process of aggradation and plains building. At or near the time of maximum aggradation, in the New Mexico region, at least, occurred the period of great basaltic lava flows. ‘These were so distributed that in some cases, the lava flowed on to the bolson plains of the great isolated valleys or into the great plains bordering the Rio Grande and other streams diverting their courses. This great period of subsidence and aggradation is most striking- ly shown in portions of southern Arizona, where Dr. W. T. Lee of the Geological Survey, has told me that the fluviatile deposits following the great eroded channelways of the Col- orado and other streams extend to several hundred feet be- low sea level as is abundantly attested by well data. While it does not seem at all necessary to postulate the great deformations of the land to account for transitions from conditions of degradation to those of aggradaation, as in many cases variations of climatic conditions including precipitation and so on, may be sufficient causes, yet where it is known that the plain of degradation extends below the plain of the present marine base level, a difference in alti- tude must be assumed. Dr. D. W. Johnson in an extensive article on the High Plains and Their Utilization, published in the 21st annual report of the United States Geological Survey, Hydrographic Division, has described with much detail the method of the formation of the frontal aprons bor- dering the mountain areas in the semi arid regions with special reference to the great sheet of Tertiary, gravels which are spread out over the high plains region, including the Llano Estacado. He presents a diagramatic section on page 729 of that report showing the relation of Tertiary gravels to the underlying Cretaceous over the Stake Plains plateau, and he rightfully, I believe, attributes their origin to the frontal ranges of the Rockies. His description of the method of formation and structure of the great Tertiary Bolson Plains of the Southwest.—Tight. 283 plains is in accordance with the writer’s views upon the same subject, and present the conditions which prevail throughout the western plateau and great basins region during a portion of Tertiary time. That there is certainly a great similarity in the method of formation of the Tertiary deposits over the Llano Esta- cado and great bolsons of New Mexico, and the basin region there is no question. The same attitude of the land under uniform climatic conditions produced throughout the entire southwestetrn country more or less uniform phenomena of erosion and aggradation on the pre-existing land forms, but that the term bolson is to be applied to any and all portions of these deposits wherever found is to be much questioned. The same conditions which spread out a great sheet of gravels over the surface of the Cretaceous on the Llano Es- tacado produced an extensive filling in all the great moun- tain-bordered basins and erosion valleys of the plateau re- gion. 7 Nor can we class as bolsons such plains of recent origin as occur along the Rio Grande, which have been described by Dr. Herrick, in the GEoLocisT, vol. 33, June 1904, as clino -plains. If we are to consider the section of the Rio Grande be- tween Bernalillo and Socorro, the Jornado del Muerto, and the Mesilla valley as typical bolsons as described by Mr. Hill, and are also to consider the Roswell basin of the Pecos as a typical bolson, it seems certain that the Roswell bolson, so classified, must be of a much more recent origin than those of the Rio Grande, for the Rio Grande deposits seem to be correlated in time with the great Tertiary deposits over the surface of the Llano Estacado, while the deposits occupying the Roswell basin have been made since the erosion of that basin out of the Tertiary and Cretaceous formations of the Llano Estacado. Again if we are to con- fine our definition of the term bolson to plains formed with- in the structural valleys (using this latter term in a very broad sense )then we must exclude the Roswell valley from the class of bolsons, for the writer is satisfied that the sec- tion of the Pecos included within the borders of New Mex- ico is wholly an erosion form. 284 The American Geologist. November, 1905 In no sense then can the extensive bolsons of New Mexico be grouped into a common class and referred to as remnants of the early Cretaceous peneplain preserved “merely by lack of erosion agencies.”’ We must then take sharp issue with Dr. Keyes, when he says of the bolsons of New Mexico: ‘“Bolson plains may be considered as sec- tions of an upraised peneplain surface in its earliest infancy, in the stage when they are as yet untouched by stream action.” As a bolson plain is a constructional form and is not confined necessarily to any period of time it must be recog- nized that the bolson plain passes through a history of con- struction and destruction similar to that of any other con- structional topographic form, and the various stgaes of its formation and destruction should be carefully noted. After the formation of the bolson plain the region may become subjected to intense erosion, which would eventually leave but remnants of the old plain, while a neighboring plain not subjected to such treatment might persist or even continue to develop its characteristics as a distinct physiographic type. It seems to the writer that the bolson plain will find its proper place and recognition in the literature of topographic forms, Glacial Lakes and Marine Submergence—Upham. 285 GLACIAL LAKES AND MARINE SUBMERGENCE IN THE HUDSON-CHAMPLAIN VALLEY. By WARREN UPHAM, St. Paul Minn Very important studies of the Quaternary history of the Hudson-Champlain valley have been recently published by Charles E. Peet and J. B. Woodworth, who have worked mainly, both in the field and in the study, without collabora- tion together, yet reaching closely similar conclusions.* The work of Mr. Peet is a continuation from his service since 1893 on the Geological Survey of New Jersey, for which he mapped the Pleistocene deposits of the Palisade Ridge, bordering the Hudson river. His plans for extend- ing this investigation along all the valley north to lake Champlain and the St. Lawrence were made under the direction of Prof. R. D. Salisbury, and the field work and presentation of results have been directed by Prof. T. C. Chamberlin; but the author claims the full responsibility for the opinions expressed. He had reached the main re- sults some four years ago, and later gave attention chiefly to the crustal movement and the origin of the water body in the Hudson valley, whether lacustrine or marine. Professor Woodworth gives in his two very elaborate publications the results of his surveys for the New York State Museum during the years 1900 to 1903, with the aid of field notes and advice by G. K. Gilbert from several seasons of his work in the St. Lawrence valley, where he had examined the country from lake Ontario around the northern slopes of the Adirondacks and southward on the west side of lake Champlain to West Chazy. That explor- ation led to the selection of the Mooers quadrangle for de- tailed mapping of its glacial drift and lacustrine and marine formations. * Glacial and Postglacial History of the Hudson and Champlain Valleys, by CHARLES EMERSON PEET; reprinted (1904), with slight revision, from the Journal of Geology, vol. xii, pp. 415-469, 617-661, July-August and October-November, 1904; with 27 figures in the text (maps, sections, pro- files, and views from photographs). Pleistocene Geology of Mooers Quadrangle, being a_ portion of Clinton County, including parts of the towns of Mooers, Champlain, Al- tona, Chazy, Dannemora, and Beekmantown, N. Y., by Jay BAcKUS WoopworiH (Bulletin 8, New York State Museum), June, 1905; pages 60, with 25 plates (maps, and views from photographs), and a folded map of the Glacial geology of Mooers Quadrangle. Ancient Water Levels of the Champlain and Hudson Valleys, by Jay Backvs WoeopwortH (Bulletin 84, New York State Museum), July, 1905; pages 65-265, with 28 plates (maps, profiles, and views), 24 figures in the text, and the Glacial map of the Mooers Quadrangle (the same ag in the preceding bulletin). 286 The American Geologist. NL In deference to McGee, Salisbury, and others, who re- gard the Lafayette and Columbia formations of the Atlantic coastal plain in southern New Jersey, and thence south to the Gulf of Mexico, as of marine deposition, Peet states very fully the arguments that would refer the Late Glacial water body in the Hudson valley to incursion of the sea. This would seem indeed to be the first and most obvious pre- sumption, in view of the fossiliferous marine beds in the Champlain and St. Lawrence valleys at altitudes ranging to a maximum of 560 feet on Mt. Royal, at Montreal, while the divide between lake Champlain and the Hudson river, near Fort Edward, is only 147 feet above the sea level. But no marine fossils are found in the abundant strati- fied gravel, sand, and clay deposits of the Hudson valley, _ which indicates, with the evidences of Quaternary uplift of - the southern part of this valley and of the Long Island re- gion and the southern Atlantic coast, that a land barrier on > the south held a glacial lake in the Hudson and Champlain valleys, outflowing along the now submarine continuation of the course of the Hudson outside the Narrows. This ex- planation of the submerged shallow valley and of the modt- fied drift and later stratified beds along the Hudson river, belonging to the time of recession of the continental ice- sheet, I have presented in various publications during the past fourteen years, having in 1892 given the name Hudson- Champlain to this glacial lake.* In other papers I have argued against the supposed marine origin of the Lafayette and Columbia series, attrib- uting them instead to river deposition on land areas, from erosion of the Appalachian mountain belt at times when that region has undergone epeirogenic uplifts.* Although a marine or estuarine origin of the Hudson valley deposits is argued by Peet as fully as seems possible, he also gives full consideration to the evidences for the freshwater deposition of these beds, evidently deeming this the more probable view, so that he leaves this question open and undecided. *(Geol. Soe. of America, Bulletin, vol. iil, pp. 484-487. * Am. Jour. Sci., third series, vol. xli, pp. 33-52, Jan., 1891. Am. Naturalist, vol. xxviii, pp 979-988, Dec., 1894. Proc., A. ‘A. A. S., vol. xliii, 1894. Compte Rendu du Congrés Géologique International, Zurich, 1894, pp. 238-251. Am GeroLoei-r vol. xxv, pp. 318-314, May, 1900. Glacial Lakes and Marine Submergence—Upham. 287 Woodworth takes more definite ground in support of the explanation of the Hudson beds as sediments of a glacial lake, to which he gives the name Lake Albany; and the glacial lake of the Champlain valley, which he thinks to have been later and distinct, he names Lake Vermont. To the present writer, however, it seems quite certain that the glacially dammed water bodies of these two parts of the Hudson-Champlain valley were continuous at the same levels, changed with the gradual northward uplift of the valley, forming deltas and shore lines which are interrupted by conditions of topography and sedimentation, but which by exact surveys with levelling will be traced continuously from the Hudson valley northward around the marine area of the Champlain,, St. Lawrence, and Ottawa basins, lying at higher altitudes than the marine shores and fossiliferous beds. By my examination, in 1901, of the lowest part of the water divide between the Hudson and the Champlain, pub- lished in the AMERICAN GEoLoGIsT for October, 1903, I could find no evidences of outflow there from the glacially ponded waters of the Champlain basin. ‘That divide or low- est place of the watershed, near Fort Edward, seems to me to have been covered by the Hudson-Champlain glacial lake, and by the later glacial Lake St. Lawrence, until the con- tinued departure of the ice-sheet far north allowed the sea to come into the St. Lawrence and Champlain valleys, then filling the southern part of the latter nearly to the hight of this col of its watershed. The names Lake Albany and Lake Vermont, applied by Woodworth, seem to be synonyms of my previous nomen- clature as lakes Hudson-Champlain and St. Lawrence, pub- lished in my U. S. Geological Survey monograph of Lake Agassiz and in other papers,* which, however, are not in- cluded in the extended bibliography given by Woodworth for this subject, although he cites a large number of my * Geol. Soc. of America, vol. iii, pp. 484-7, 1892. Am. Jour. Sci., third series, vol. xlix, pp. 1-18, with map, Jan., 1895. Minnesota Geol. and Nat. Hist. Survey, Twenty-third Annual Report, for 1894 (pub. Feb., 1895), pp. 156-193, with map. U. S. Geol. Survey, Monograph xxv, The Glacial Lake Aggassoz, 1895, pp. 254, 262-264. Am. GEoLoGcisT, vol. xxxii, pp. 223--230, Oct., 1908. International Quarterly, vol. xi, pp. 248-265, July, 1905. 288 The American Geologist. Nevemiety ous earlier glacial papers. Several very noteworthy papers by others, also, as Elias Lewis, Jr.,t and Prof. J. S. Newberry,t relating to Long Island and the Hudson valley, are similarly overlooked in his bibliography. From consideration of the amount and probable rate of the rise of the Champlain and St. Lawrence region from the Late Glacial and Postglacial marine submergence, Woodworth estimates the duration of the Postglacial epoch as somewhere between 20,000 and 100,000 years. ‘The pres- ent writer has shown, however, that nearly all the uplifting of the Lake Agassiz area took place probably within so short a time as about one thousand years, during the ex- istence of that lake, since which time the region has been affected only by very slight changes of level. Likewise probably the uprise of the St. Lawrence basin was at first relatively rapid, so that it might all take place within the period of about 7,000 or 6,000 years which is indicated for Postglacial time in that part of the northern United States and Canada by Prof. N. H. Winchell in his studies of the recession of the Falls of St. Anthony, with which my studies of the Niagara falls and gorge well coincide. The former estimate of the period since the Ice age as tens of thousands of years, still advocated by Gilbert and Woodworth, is op- posed by a great range of well accordant evidences on the glaciated areas of both North America and Europe. This Hudson-Champlain area, made classic in glacial geology by the work of C. H. Hitchcock, Baldwin, Baron de Geer, Gilbert, Merrill, Peet, Woodworth, and. others, which through the writings of Hitchcock and Dana gave the name Champlain to the closing epoch of the Ice age, deserves yet further work of detailed surveys, with exact levelling for determination of the relations of all its lacustrine and marine shore lines. No other area of our continent promises more important information concerning the Glacial and Recent periods. It should also be added that the deeply submerged outer fjord of the Hudson, made known with exact soundings and charting by Lindenkohl, is the key to the causes of the Pop. Sci. Monthly, vol. x, pp. 434-446, Feb., 1877. Pop. Sci. Monthly, vol. xiii, pp. 641-660, Oct., 1878. tr sb The Jurassic Horizon.—Keyes. 289 Glacial period, by its testimony of very great preglacial land “elevation, together with the similar evidence given by the submarine continuations of the Congo, the Adour, and other -fivers, and by the profound depths of the Scandinavian and | Arctic - fjords. eal JURASSIC HORIZON AROUND THE SOUTHERN END OF THE ROCKY MOUNTAINS. By CHARLES R. KEYES, Socorro, New Mexico Soon after passing the Colorado line the Rocky moun- tains rapidly lose their predominant characteristics and fade out completely into the Mexican tableland. The moun- tain ranges which succeed to the southward are short, iso- lated, tilted blocks, that are of a wholly different type from that of the mountainous structures to the northward, and to which they present marked topographic contrasts. At this southern extremity of the Rockies in northern New Mexico, the general stratigraphy presents some un- looked for phases that are of exceptional interest. More- over, it is here that the eastern Mississippi valley strati- graphy, with which American workers are most familiar, loses its identity and is replaced by a less known western stratigraphy. The rock-successions of these two provinces have never been satisfactorily or exactly paralleled. Of the ‘many stratigraphic problems that have arisen recently for solution in this region none has possessed greater interest than the questions surrounding the horizon at which the Jurassic system should be represented. Ever since the time of Jules Marcou’s trip, sixty years ago, in connection with the Pacific railroad expedition along the thirty-fifth parallel, when he pronounced the now cele- brated Tucumcari section in eastern New Mexico as of Triassic and Jurassic ages, there has been waged one of the bitterest and most useless controversies in the history of American geology. Marcou was well acquainted with’ Ju- - rassic and Triassic sections of Europe and, as Louis Agassiz has well remarked,* he could hardly be blamed for seeing * Am. Jour. Sci., (1), vol. xxvii, p. 134, 1859. 290 The American Geologist. NON CHER eres a close analogy in the New Mexican sequence. The full force of this position finds another instructive parallel in the so-called Permian question of central Kansas. Both of these controversies doubtlessly would have been avoided had all participants relied less on analogy and more upon the actual critical criteria which the formations themselves supply. Singularly enough, after all these years in which Mar- cow has stoutly maintained the correctness of his original position, the “Triassic” part of the Tucumcari section ap- pears finally to be determined without much doubt as Tri- assic in age. It now,becomes a question of more than passing interest to inquire anew regarding Marcou’s Jurassic beds of the same locality. -According to Marcou’s Pyramid mountain section, which is near the Cerro Tucumeari, and which is essentially the same, there were included in his so-called Jurassic sequence (a) about 225 feet of soft, shaly, light-colored sandstones, which Hill has since correlated with the Trinity sands of central Texas, (b) 50 feet of bluish fossiliferous shales, which Hill considers as forming the uppermost por- iton of the Washita division of the Comanche series, and from which Marcou collected his few fossils, and (c) 50 feet of massive yellow calcareous sandstone, which has since been found to be the attenuated extension of the Dakota sandstone. Even within the last decade Cummins has gathered all of these beds into a single unit and proposed for them the-title of the ~ Tucumcari formation-> 7 Allgot these formations at Tucumeari appear to form a perfectly conformable succession. More extended observations have lately shown quite conclusively that marked unconformities actually exist be- tween everyone of the formations mentioned. Regarding them many questions now arise concerning their real sig- nificance in the geological history of the region. The remnant of the Dakota sandstone (c) which is found in the Tucumeari section is now known to form the base of the Mid-Cretaceous (Upper Cretaceous of Meek ~ Journal of Geology. vol. vii, pp. 221-241, 1899. * Texas Geol. Sur., Third Ann. Rept., p. 201, 1892. The Jurassic Horizon. —Keyes. 291 and Hayden). It rests unconformably on all older forma- tions, from the Mid-Carboniferous limestones to the Comanche series. The shale (b) beneath the massive sandstone at the top of the Tucumcari section, has been correlated with the top- most portion of the Washita division of the early Cretaceous as represented farther to the eastward in Texas. The lower members of the early Cretaceous successively thin out to the north and west from the central part of that state and each overlaps the next below. The next formation below (a), which rests unconform- ably upon the Triassic Red Beds and which has been par- alleled with the Trinity sands of central Texas appears to be a formation with as yet no tangibly determinable rela- tionships. It may be the basal member of the early Cre- taceous section which is so well developed farther to the eastward, and this has been the view advanced by Hill and other workers in the Texas field. Or, it may be a littoral deposit that followed up an advancing shore; and thus it may have an age in its different parts extending throughout the Comanche period. However, this phase of the subject. receives full discussion elsewhere. This so-called Trinity sandstone stands apart from all else. It has no direct genetic relationships with the forma- tions either above or below. The unconformable relations that it bears both to the superior strata and to the inferior rocks clearly indicates the lapse of a considerable time in- terval at least at the base. There is then in this sandstone an important geological formation about which little is yet definitely known regarding its geological relationships ; and to the westward at the same horizon an important erosion interval is represented. The equivalents of these in the sediments of other localities, as well as the space they repre- sent in the general geological column have become topics of some speculation. White, who was long the best American-authority on the Cretaceous rocks, considered the Trinity sands, or Dinosaur beds, as reaching down into the Jurassic period. Marcou regarded the Jurassic as partially represented by this formation. Most writers have disputed the existence 292 The American Geologist. Nercines aes of any Jurassic beds in this part of the continent. Their evidence has been even less conclusive than that presented by the pioneer geologist just mentioned. It is now known that Marcou and his critics were not discussing exactly the same thing. Independent of whatever may have been concluded in the past regarding the presence or absence of Jurassic de- posits in the Tucumcari section it is certain that there exists at the horizon where the Jurassic system is naturally lo- cated in the general geological column, a stratigraphic gap and a formation about which there is much to learn before their real significance is understood. It may be that after all Marcou’s surmise was right and that the Jurassic sys- tem finds representation in the Cerro Tucumcari, just as it now appears that his shrewd guess regarding the Triassic eventually proved to be correct. In this connection it is of interest to note that in west- ern New Mexico, in the-Zuni region, Dutton has regarded the great sequence of sandstones which he called the Zuni series, and which is upwards of 1,200 feet thick, as very likely of Jurassic age. He correlated this series with the extensixe deposits of so-called Jurassic age in Arizona, Utah and southwestern Colorado. The Zuni series for the pres- ent is here still associated with the Triassic system. Its stratigraphic relationships, especially with the Dakota sandstones, and the position in the Tucumcari region are indicated in the section subjoined (Fig. ..). DAKOTA SANDSTONES THE JURASSIC HoRIZON IN THE SOUTHERN ROCKY MOUNTAINS. The horizon represented by the heavy line is worthy of much attention. Its stratigraphic horizon is that of the Jurassic system of the general geological section. a. Ff - UNIVERSITY of ILLINOIS: = 7 / } . e * = ’ \ , , ~— 6 a * ad - PLATE XV THE AMERICAN GEOLOGIST, VOL, XXXVI INSTITUTO GEOLOGICA DE MEXICO El Instituto Geologica de Mexico.—-Guild. 203 EL INSTITUTO GEOLOGICA DE MEXICO. By F. N. GuiILp, Tuscon, ARIZ. PLATE XV. Since the International Congress of Geologists is to convene in the city of Mexico during the coming summer of 1906, it may be interesting to the readers of the AMERI CAN GEOLOGIST and especially to those who expect to attend the congress, to learn something of the work of the Institute in Mexico which corresponds to our national geological sur- vey. Such a description seems especially opportune at the present time when the Institute has taken up its quarters in an excellent new building expressly designed for its pur- poses, and is now busily engaged in sending invitations to all parts of the world and making other preparations for the congress which is to be held within its walls. The first step which led to definite results in the forma- tion of a geological survey in Mexico was made in 1886 and through the efforts of Antonio del Castillo, then professor of mineralogy and geology in the School of Mines, an au- thorization was obtained two years later for the formation of a Comision Geologica de México. The first publication issued in 1895 appeared under the title of Boletin de la Comision Geologica de México. Later, however, the name was changed to Instituto Geologico National de México and the publications appeared under that name. Castillo, who may be considered as the founder of the Institute, was chosen director which position he held until his death in 1895. One of the first objects of the Institute seems to have been the preparation of sketches (bosquejos) on the gen- eral geology of the country. These appear in bulletins No. 4, 5, and 6. They are accounts of scientific expeditions by various members of the staff into different parts of the re- public. ‘oh - The Institute was first housed in the School of Mines building, later however, removed to temporary quarters in the Calle de Paseo Nuevo Num. 2, and finally into its pres- ‘ent building on 5a Calle del Ciprés. It is equipped with excellent chemical laboratories for the analysis of rocks and minerals, museums for geological and mineralogical collec- tions, drafting rooms, libraries, laboratories for microscopic 204 The American Geologist Nesemen Tees investigation, and all necessary appliances for geologic re- search. The museum is especially well equipped with a large collection of nicely trimmed rocks and thin sections corresponding. Possibly there is no better place than Mexico for the study of variations in rhyolitic and andesitic outflows, and the Instituto Geologico keeps its doors open to scientists who desire to study there. The staff of the Institute at present consists of José G. Aguilera, appointed director on the death of Castillo, Ezequiel Ordonez, sub- director and petrographer, Emilio Bose, Carlos Burckhardt, Juan D:; Villarello; E.sAngermann; TF lores, R.Roblesss: Truax, and A. Villafana, geologists, R. Santillan, secretary, F. Roel, and V. de Vigier, chemists. The Institute has an interesting and in some respects unique field for investigation. The larger portion of the sedimentaries and older crystalline rocks in Mexico are cov- ered by great masses of recent products of volcanic activity such as ashes, andesitic and basaltic outflows. The Insti- tute has a very complete collection of these rocks which have quite thoroughly been worked out from a petrograph- ical standpoint and presented to the public through its ex- cellent bulletins. Its investigators plan in the near future to discuss more completely the chemical relations of the outflows and doubtless valuable additions will be made to our knowledge of the differentiation of volcanic magmas. Volcanic craters are found everywhere, some in the state of activity (Colima) others possessing but faint traces of their formet power (Popocatepetl). Even within less than two hours ride from the city of Mexico groups of volcanoes may be studied where crater cones rise but a few hundred feet above the level valley of Mexico (Sierra de Catarina.) These present variations from pure cinder cones (Las Cal- deras) to cones from the crater of which more liquid mate- rial has escaped (Cerro de Ixtapalapa). Thus a more ideal spot for the investigation of at least one phase of geology could hardly be imagined. Following is a list of the publications of the Institute: Num. 1.—Fauna Fosil de la Sierra de Catorce, por A. del Castillo y J. G. Aguilera.—1895.—56 pp., 21 1am. Num. 2.—Las Rocas Eruptivas del S. O. de la Cuenca de México, por E. Ord6nez.—1895.—46 pp., 1 1am. El Instituto Geologica de Mexico.—Guild. 205 Num. 3.—La Geografia Fisica y la Geologia de la Peninsula de Yu- catan, por C. Sapper.—1896.—58 pp., 6 lam. Nums. 4, 5 y 6—Bosquejo Geol6gico de México.—1897.—272 pp., 5 1am. Nums. 7, 8 y 9.—El Mineral de Pachuca.—1897.—184 pp., 14 lam. Num. 10.—Bibliografia Geologica y Minera de la Republica Mexicana por R. Aguilar y Santillan.—1898.—158 pp. Num. 11.—Catalogos sistematico y geografico de las especies mine- ralogicas de la Republica Mexicana, por José G. Aguilera.— 1898.—158 pp. Num. 12.—E] Real del Monte, por E. Ordonez y M. Rangel.—1899. —108 pp., 26 1am. Num. 13.—Geologia de los alrededores de Orizaba, con un perfil de la vertiente oriental de la Mesa Central de México, por Emilio Bose.—1899.—78 pp., 3 lam. Num. 14.—Las Rhyolitas de México (Primera parte), por E. Ordé- nez.—199.—78 pp., 6 lam. Num. 15.—Las Rhyolitas de México (Segunda parte), por E. Ord6- nez.—1901.—78 pp., 6 lam. Numero 16.—Los Criaderos de fierro del Cerro del Mereado en Du- rango, por M. Rangel, y de la Hacienda de Vaquerias, Estado de Hidalgo, por J. D. Villarello y E. Bose.—1902—144 pp., 5 lam. Numero 17.—Bibliografia Geol6gica y Minera de la Republica Mexi- cana por R. Aguilar y Santillan.—i904. [E£n prensa.] PARERGONES. Tomo I. No. 1.—Los temblores de Zanatepec, Oaxaca.—Estado ac- tual del Volcan de Tacana, Chiapas, por Emilio Boése.—1903. 25 pp., 4 lam. No. 2.—fisiografia, Geologia 6 Hidrologia de los alrededores de la Paz, Baja California, por E. Angermann.—E] Area cubierta por la ceniza del Volcan de Santa Maria, Octubre de 1902, por Emilio Bose.—1904. 26 pp., 3 lam. No. 3.—E] Mineral de Angangueo, Michoacan, por BH. Ord6nez.—Ana- lisis de una muestra de granate del Mineral de Pihuamo, Ja- lisco, por J. D. Villarello—Apuntes sobre el Paleozoico en So- nora, por HE. Angermann.—1904. 34 pp., 2 lam. No. 4.—Estucio de la teoria quimica propuesta por el Sr. Andrés Almaraz para explicar la formaci6n del petréleo de Aragon, México, D. F., por J. D. Villarello.—E1 fierro metedrico de Bacubirito, Sinaloa, por E. Angermann.—Las aguas subterra- neas de Amozoc, Puebla, por E. Ord6énez.—1904.—24 pp., 1 lamina. No. 5.—Informe sobre el temblor del 16 de Enero de 1902 en el Esta- do de Guerrero, por los Dres. E. Base y E. Angermann.—Es- tudio de una muestra de mineral asbesti‘orme procedente del Rancho del Ahuacatillo, Distrito de Zinapécuaro, E. de Michoa- can, por el Ing. J. D. Villarello.—1904.—26 pp. 296 The American Geologist. November, 1905 No. 6.—Estudio de la hidrologia subterranea de la region de Caderey- ta Méndez, EB. de Querétaro; por el Ing. J. D. Villarello.—1904. —58 pp., 2 lam. No. 7.—Estudio de una muestra de grafita de Ejutla, Estado de Oaxa- ca, por el Ing. J. D. Villarello.—Andalisis de las cenizas del vol- can de Santa Maria, Guatemala, yor el Ing. E. Orddénez.— 1904.—26 pp. No. 8.—Hidrologia subterranea de los alrededores de Querétaro, por el Ing. J. D. Villarello.—1905.—56 pp., 3 laminas y 2 figuras. ‘City of Mexico, Aug. 25, 1905. ‘SSERPENTINES IN THE NEIGHBORHOOD OF PHILADELPHIA. ANNA JI. JoNAS, Bryn Mawr, Pa. The object of this paper is to give a brief review of the occurrence and origin of the known serpentines, and to describe in particular, the serpentine dykes in the neigh- borhood of Philadelphia, Penna. It is generally conceded that serpentine, wherever oc- curring as a mineral or a rock, is a secondary product formed in the zone of katamorphism and that it is devel- oped by the alteration of non-aluminous, ferro-magnesian silicates ; olivine, the pyroxenes, anthophyllite, tremolite and actinolite. In a less number of cases serpentine has been derived from a limestone. An entire rock mass may be composed exclusively of serpentine, or the rock may contain remains of the original minerals from which the serpentine was derived. The physical characters of the rock serpentine are therefore somewhat modified by the presence of associated minerals. In color serpentine has a wide range through all shades of green, brown and reddish brown. Its texture depends largely on the mineral from which it was derived; serpen- tine formed by the hydration of olivine is massive; that variety formed by the alteration of an amphibole is usually fibrous. That variety which results from the alteration of pryoxene may be described as massive. Since serpentine, a katamorphic product, is not easily weathered, it usually forms a ridge scantily covered with a sterile soil composed of silica, magnesia and stained with iron oxide. Serpentines Near Philadelphia --Jonas. 207 Distribution.—Serpentine has a wide distribution through the British Isles and Europe, and has been describ- ed from several localities in Asia and Africa. The serpen- tines of England, Wales and Scotland have been traced to olivine rocks and are usually associated with masses of gabbro or dioryte. The serpentines of Europe, for the most part, occur in belts of igneous rocks and crystalline schists and gneisses, and are largely derived from perido- tytes, pyroxenytes or gabbros. Serpentinised marble is re- reported from the Passauer gneiss district of central Europe, from the upper Reno valley of Italy and from the Knopia district of Finland, and serpentine is associated with cal- careous schists on Corsica and at Antioch, Asia. In America serpentine is found throughout the belt of crystalline formations which extends from Maine to Ala- bama and forms the floor of the Piedmont plateau. Maine.—*In Maine, serpentine has been reported by Mr. George P. Merrill at the northern end of Deer Isle in Penobscot bay. He describes it as a very dark green varie- ty mottled by diallage crystals. Vermont.—There are many localities of serpentine in the state of Vermont? on the boundary between Dover and Newfane counties, at Windham; in the hills of the north- western part of Chester extending to Ludlow and Caven- dish; at Plymouth, Roxbury, Westfield and Troy. The serpentine is associated with steatite and occurs both in mica schists and gneisses. It is placed among the strati- fied rocks because it occurs as thick beds in foliated rocks and does not cut them. This could be accounted for on the supposition that the serpentine was an intrusive which had been folded along with the rock into which it was intruded. The steep slopes of Belvidere? mountain are composed of amphibolyte. In it the hornblende has been largely alter- ed to fibrous serpentine. Massachusetts.—In the Holyoke folio Emerson dis- cusses the serpentine which extends from Holyoke, Massa- chusetts, south into Connecticut. The Chester amphibolyte *G. P. MERRILL, ‘Stones for Building and Decoration,” p. 60. + Geology of Vermon 1861, vol. i, p. 544. t Science, vol. xxi, No. 533, Mar. 17, 1905 (review). “The Serpentine a Associated Minerals of Belvidere mountain, Vermont,” by V. F. ARSTERS. 298 The American Geologist. November ieee is described as a ‘dark, flaggy hornblende schist,” in part replaced by serpentine and emery. In an earlier publica- tion it was described as an altered eruptive, but in this folio Emerson calls it an altered sediment, probably a dolomyte and of Lower Silurian age, lying between the Rowe and Savoy schists, both of which are sericite schists. Emerson decided that the Chester amphibolyte is a sediment because in the sedimentary series of Connecticut, Massachusetts and Vermont there are beds of dolomyte which pass into ensta- tite limestones and amphibolytes. Not only is emery found in limestones but the amphibolytes of the above mentioned series are derived from limestones. The Pelham gneiss* is exposed in long, narrow strips, extending north and south and lying to the east of the Connecticut river in Pelham and Shuttesbury. In this gneiss are dykes of a bronzite- olivine rock partially altered to serpentine. In this monograph Emerson mentions the occurrence of serpentine in the Chester amphibolyte. It enters Massa- chusetts from Vermont and extends southwest through Rowe, Hampshire, Hampden, Blauford, Granville and Russel counties and dips below the sands of the Westfield plain and does not reappear. New Yorp —I\n 1887 Dr. Williams published a paper on the serpentine? in the Onondaga salt group at Syracuse. The exposure was situated on James street but for many years has been inaccessible. It was noted in 1837 and re- ported to Vaunuxem, the state geologist, who regarded it as an aqueous deposit. Dr. Williams claims for it an igneous origin $ in 1890 he published some additional proof for his view. $8 In Essex county at Port Henry and Moriah, there is serpentine derived from an altered dolomyte and pyroxene limestone. ) -Mi- eroscopic character of the ore of the Treadwell mine, Adams, Iv. 88: Mt. St. Elias, Russell and Yukon valley, Hayes, (abs.), lv; 216; Ice under tundra, Russell (p.s.n.), vi 325; Ice cliffs on the Kowak river, Cantwell, vi, 51; Explorations in, Anon, vil, 33; Muir glacier, H. P. Cushing, viii, 200 SDICtoy {Gon Hh eseVVl SiGe Millie 330; Pribyloff islands, S. Brown (rev.) Ix, 217; Alaska, John Muir, tosi Soc. (p. xi, 287; Physical geography of, Russell (rev.) xiv, 331; Geology of Glacier bay, Cushing (abs.), XV; Gls) (Ditto) (reve xvii, oe Hypersthene-Andesite from Mt. Edgecombe, Cushing, xx, 156; Explorations (p,s,n,), xxi, 265; Reconnoissance of gold fields, G. FW. Becker (rev.), xxi, 382; Sur- face geology, O. Nordenskjold, xxlii, 288; Crossing the Valdez glacier at Bates pass, W. R. Abercrombie, xxiv, 349; Work of the U. S. Geol. Sur. (p.s.n.), xxvl, 64; Scapolite rocks, J. E. Spurr (rev.) xxvi, 393; Granite of the Yukon valley, R. G. McConnell, xxx, 55; Extinct bison (p.s.n.) xxxi, 262; Harriman Expedition, Glaciers and glaciation, G. K. Gilbert (rev.), xxxiii, 259; Dit- to, Geology and _ paleontology, Emerson, Palache, Dall, Ulrich, Knowlton (rev.), xxxiv, 122; Coal December, 1905. fields (p.s.n.) xxxiv, 401; Recon- noissance in northern, Schrader, (rev.) xxxv, 247. Albertite-like asphalt in the Choc- taw nation (rev.) xxiv, 319. Alden, W. C. (with R. D. Salis- bury), Geography of Chicago and its environs (rev.), xxv, 174; Chi- cago, folio, U. S: G. S., sexx, 255. Alderson, V. C., Geology in the High School, iv, 284. Algae, Considerations on, G. Mail- lard (rev.) ii, 54; From the Tren- ton limestone, R. P. Whitfield, (rev.), xv, 188;. As geological guides, xili, 95. Algérie, Le bassin de la Tafna. L. Gentil, (rev.), xxx, 253. Algonquin and Nipissing beaches, F, B. Taylor, xvii, 397; and War- ren beaches. Upham, xvll, 400. Algonquin river. G. _ K. -Gilbert (abs.), xviii, 231, Alkali deposits of Wyoming, ty ae Read, xxiv, 164. Alkaline rocks of Madagascar, A. Lacroix (rev.), xxxi, 183. Alkaline reaction of some natural silicates. F. W. Clarke. (rev.), xxiii, 328. Allamakee county, Report on. S. Calvin. (rev.), xvil, 51. Allanite and Epidote, intergrowths of, W. H. Hobbs, xii, 218. Allegany county, Maryland, Abbe and O’Harra (rev.), xxix, 119. Allen, Thos. W., (p.s.n.), xxvii, 327. Allotropic forms of silver. Lea (eit.), iv. 254. Alluvial river terraces, develop- ment of (rev.), R. E. Dodge, xlv, 97. Altitudes between lake Superior and the Rocky mountains, Upham (rev.) ix, 341; Dictionary of, in the United States. Gannett (rev.) xxv, 121. Aluminum, produced by electroly- sis (p,s.n.) iii, 844; Market prices (p.s.n.) vii, 272. electro-metal- lurgical process (p.s.n.) x, 398. Alunogen and bauxite in New perce (abs.) W. P. Blake, xiv, Amboy clay series, Age of, A. Hol- leks (abs); ) exXxit, ee eDo. America, How long ago peopled, (ed. com.), xxxi, 312 American Anthropological associa- tion (p.s.n.), xxxvi, 64. American Anthropologist (p.s.n.), y 183; (rev.), ili, 149: American Aphidae, Tertiary. Scud- der. (rev:)} xv, 123: American Association for the ad- vancement of Science (ed. com.), lip) dis ACpisen)h litielsss soogsGpe Sin:), ive)104,) 2515 25620 (p Sena) au wile 261; (p.s.n.), viii, 62, 192; Pleisto- cene papers at, viii, 230; (p.s.n.), xii, 130; Pleistocene papers at, xii, 172; (p.s.n.), xii, 207; Lists and abstracts of papers, xiv, 202; (p.s.n.), xv, 195: (p.s.n.), xvi, 68; Geol. Soc. and Am. Asso., War- ren Upham, xvi, 233; (p.s.n.), xviii, 59; Warren Uphm, xviii, Index, yee (usin); xxi, 333°. (pis-n:), xxii, 130; Geology and ‘eogra- phy, Upham, xxii, 248; (p.s.n.), xxiv, 197; Sketches of past pres- idents by. Marcus Benjamin (p. Retin) ei, O90; (p.S.n:), | XXV, 394; (p.s.n.), xxvii, 387; Commem- orative tablet (ed. com.) xxix, Ties) -s:D.),) XXX, 398; (p/s.n.) xxxl, 66; Summer meeting of Section EH, 1905, E. O. Hovey, xxxv, 398; (p.s.n.), xxxvi, 331. American committee of the Inter- national Congress of Geologists. Pp. Erazer,’ i; 3, 86; Report on the several formations, i, 97; Re- ports of the American Commit- tee, ii, 189; An unjust attack up- on, P. Frazer, iii, 65. American Géologist, Introductory, I, 1; Consolidation with Economic Geology, xxxvi, 309. American geological classification and nomenclature, J. Marcou, (rev); “il, 129. American Geological railway guide, Macfarlane (rev.), vi, 248. American Geological Society, Pro- posed, i, 394; (p.s.n.), ii, 360, 370; (p.s.n.), iii, 62, 140, 344. See Geo- logical Society of America. American Institute of Mining En- gineers, -(p.s.n.), xvi, 268, 330; Gps.) EXVil, a aD; 5) (P-Sem.)s x1; ZUM SMe), XXX, 202, (DeS-M.), 65, BOL DsS. Te). XXXII, 264: American meteorites described (p. s.n.), xxviii, 265. American Meteorological (rev.), xi, 357. American mining congress (p.s.n.), xxii, 400 American Museum of Natural His- Journal, tory (p.s.n:); xxiii, 395; (p.s-n.) xv O42 1(p:Sin-) > xxvii, 64; (Cpis:. Nays xxVvil, soos (P:s.n.). xxix, 130; Progress of vertebrate paleontol- SV! belay, Xxxv;. 31: American Naturalist, (p.s.n.), i, 134; v, 255. American Paleontological Society, SecA, OF PP; Bay, xxxv, 124: American petrographical micro- scopes, N. H. Winchell, iii, 225. American Philosophical Society (ed. com.), xxviii, 317. American Society of Naturalists (pis. Sel; 1383. American Society of Civil Engin- G€ersin(p sin) vs. 127. American Neocomian and Gryphaea pitcheri. Marcou, v. 315. Ames knob, North Haven, Maine, Halley Willis, xxx, 159. Ami, H. M., List of fossils of the Quebec (rev.), v. 247; The Citadel Hill rocks (p.s.n.), vii, 71; Strata of the Quebec group (rev.), viii, 115; Geology of Quebec and its environs (rev.), viii, 186; Cam- brian fossils from the Rocky Mt. TOP CADS.);_1:Xts 0 182: Quebec group about Quebec (abs.), xiv, 66; Note on a collection of Silu- rian fossils (rev.) xv, 264; (p.s.n.) Xvi, 267; Preliminary list of or- ganic _remains (rey.), xvii, 393; Ordovician in New Brunswick ~ Dawson, Volumes I-XXXVI. - 5 and Nova Scotia (rev.), xx, 276; Sketcn ur J. W. Dawson, xxvi, 1; A national muséum for Canada, xxvii, 259; Sketch of EH. Billings, XXVIII, zo: bibliography of G. M. xxviii, (6; billings and his bibliography, xxviii, 128; Bel- inurus siltorkensis, xxix, 138; Sketch of A. R. C, Selwyn, Xxx, 12) (Dp: Sai.) , ocoxxls 332: Ammoniten-Brut mit Aptychen in der Wohnkammer von Uppeha steraspis Uppel, Michael rev.) xvi, 312. Amount of glacial erosion in the Finger lake region of New York. D. #. Lincoln. (abs.) xii, 177. Ampyx, with descriptions of Amer- an species. A. W. Vogdes, xi, oh). Amusing error (ed. com.), xv, 120. Amygdaioid in Manitoba (p.s.n.), XxXxiv, 132, Amygdaloidal melaphyrs of the Boston basin, W. O. Crosby, xxvii, 324. Amyzon beds, ii, 289. Anaconda Copper Company (p.s.n.), xxvii, 197. Analysis of folds. Van Hise. (abs.) xvi, 244. Ancestry of the upper Devonian placoderms of Ohio, E. W. Clay- pole, xvii, 349. Anderson, F. M., River system of aoe California (abs.), xxvil, Anderson, C. C., Report on the wa- rea powers of ‘Georgia (rev.), xxil, 9 Anderson, J. G. Om Olandska ran- kar (rev.), xvii, 55: Cambrische u. Silurische phosphorit fiihrende Gesteine aus Schweden (rev.), xix, dar: Anderson, Netta C., List of Mas- todon and Mammoth remains (rev.), xxxvli, 258. Anderson, R. V. (p.s.n.), xxxv, 261. Ancient glacial action in Austral- asia, C. H. Hitchcock, xxiii, 252. Ancient lake beaches on the islands in Georgian bay, F. M. Com- stock, xxxiii, 312. Ancient river deposits of the Spring river valley in Kansas, O. H. Hershey, xvii, 37. . Ancient volcanic rocks of South ta (rev.), F. Bascom, xix, Andesytes of the Aroostook volcan- ic area of Maine (rev.), H. E. Gregory, xxv, 175. Animals before man in North unre F. A. Lucas (rev.), xxx, Andrews, William, The Diuturnal eaeOny of the Earth (rev.), xxv, ou. Andrews, E. C., Limestones of the Fiji islands (rev.), xxvii, 256. Andrews, C. W., Recently discov- ered extinct vertebrates from Egypt (rev.), xxviii, 389. Andrews, Edmund, Sketch of work (p.s:n.), xxxiil, 201. Animikie Black Slates and Quartz- ytes, equivalent to the Huronian 6 The American Geologist. No Eis Winchell, ci; 1h;.) Uncon-= formities of, in Minnesota, A. Winchell, I, 14; Copper in the caps rocks, A. C, Lawson, v, Anhedron, a new _ petrographical term, Ll. V. Pirsson, (abs.), xvii, 94. Annals of British Geology. J. F. Blake (rev.), xi, 302; xv, 387. Ann Arbor, post-glacial geology. Wooldridge, ii, 85; Lake beaches at Spencer, Il, 62. Annelid, new genus and _ species, S. Calvin, i, 24; Teeth from the Hamilton; ve We Clarke, lain: from the Medina, Foerste, ii, 416. Announcement of the Theory of Evolution (ed. com.), xxviii, 316. Anorthosyte as a rock term, Kolde- rup, xxxli, 392; H. P. Cushing, xxix, 190. Anorthosytes of the Minnesota shore of lake Superior, A. C. Lawson (rev.), xII, 59. Another appeal to induction from the scholastic methods of mod- ern geology. (rev.), H. H. How- orth, xxxvl, 125. Another episode in the history of Niagara river, - J. Spencer, (abs.), xxil, 259. Another Kansas meteorite. (p.s.n,), xxviil, 334. Another meteorite in the supreme court, (ed. com.), xxxvl, 47 Another old outlet of lake Huron, G. F. Wright (p.s.n.), x, 262. Antarctica (ed. com.), xvii, 241; Antennae and other appendages of Triarthrus becki, W. D. Matthew, (rev.), xl, 193. Anthracite coal, Bow river, Cana- dian Northwest, Dodge 1, 172; Geo. M. Dawson, I, 332; Exhaus- tion of (ed. com.), Ill, 45; In Col- orado, Lakes, vill, 14; Origin of, C. R. Keyes, xlil, 411; New the- ory: of origin, W. S. Gresley, xviii, 1; In Arizona, W. P. Blake, xxl, 345. ple vOltean: Martin (p.s.n.) Il, Antilles, Archean character of the nuclei, P. Frazer, xxl, 250; Slopes of drowned valleys, J. W. Spen- Cen (abs: )s oval, i 23T. Antiquity of the fossil man of Lan- sing, Kansas, Upham, xxx. 135; Ditto (ed. com.), xxx, 189; Ditto, Upham, xxxl, 25; Pleistocene ge- ology of the Coneannon farm near Lansing, N. H. Winchell, xxxl, p.. 263;. Ditto, Williston, Todd, Wright, xxxl, 291, 294; (ed. com.) xxxlIl, 185; More about, Luella Owen (rev.), xxxll, 254: Evidences of rheumatoid arthri- tis, C. A. Parker, xxxiii, 39; On the Lansing man, S. W. Willis- ton, xxxv, 342. Antiquity of man (ed. com.), Il, 51; Putnam (cit.), v, 128; In eastern N. Am.. N.S. Shaler, xi; 180: In America, W. J. McGee, xil, 174; (ed. com.), xxxi, 312; See ‘under Man. Antiquity of the races of mankind, xxviii, 250. December, 1905. Antiquities from under Tuolumne Table mountain. G. F. Becker. (rev.), “vil, 258; at Baoussé Rousse, x, 296. Apatite in Norbotten, Norway, Loesstrand (abs.) xi, 364; ecrys- tals, Antwerp, New York (rev.), N. Knight, xxxi, 62. Appalachiah Virginia, N. H. ton, x, 10; A. Keith, x, 362. Apparent anomalies of stratifica- tion in the Postville well, S. Cal- vin, xvii, 195. Appleby, W. R. (p.s.n.), viii, 404. Applied Geology, International Congress (p.s.n.), xxxvi, 62. Appomattox formation (rev.), Il, 130. Approximate interglacial chronom- eter, N. H. Winchell, x, 69, 302. Aqueous origin of gold, Everette, (p.s.n.), vii, 389. Aragonite fossil shells more solu- ble than those of calcite (rev.), I, 261. Areal geology of the Castle Rock region, Colorado, xxix, 96. Archean, The, T. G. Bonney (ed. com.), iv, 424. 5 Archean and Algonkian, changes in, by Van Hise (ed. com.), xxviil, 385. Archean geology of Missouri, Ha- worth, i, 280. 363; of the Antilles, Frazer, ii, 421; Fossil plant. Brit- ton (rey.), ii, 58; Formation of America, opinions of American geologists, report of the Amer- ican committee, P. Frazer, il, 146; Report of the English com- mittee (cit.), ii, 187; Artesian wells from in Minnesota (p.s.n.), iv, 392; Geology of the region N. W. of lake Superior, Lawson, (rev.), iv. 59; Ditto. vii, 320; Dit- to, Van Hise. vii, 383; Not to be correlated with that of Europe, Barrois (cit.), viii, 255; Eruptive rocks of Finland (ed. com.), ix, 49; Of southern Mass. (abs.), Emerson, xv. 247: Gneiss in the Sierra Nevada. xvii, 344: Lauren- tian north of Montreal. F. D. Ad- ams (rev.). xx, 131; Gneisses of the Grenville series. F. D. Adams (rev.), xx, 200; Nuclei of the An- tilles! (P) Prazer, \xxi,! 250) vRe= semblances between Minnesota and Finland. N. H. Winchell, xxi, Hee Of the Alps (ed. com.), xxviil, 89. Archaeological notes on _ central Minnesota, O. H. Hershey, xxiv, 2838. Arctic exploration (p.s.n.), xiv, 272; (ed. com.), xiv, 389; (p.s.n.), xx, He the Arctic climate, secular (ed. com.) xv. 254. Area and duration of lake Agassiz, Vill, 227. Areal work of the U. S. Geol. sur- vey, W. J. McGee, x, 377. Arenicolites, ii, 2. Argyrodite and a new sulphostan- nate of silver from Bolivia (rev.), S. L. Penfield, xiv, 53. Dar- changes Index, Arid belts of South Africa and South America, Proposed exam- eae E. W. Hilgard, xxxiil, Arietidae, Genesis of, by A. Hyatt. Jules Marcou, vi, 128. Arizona ores (ed. com.), xiii, 419; Petrified forest (p.s.n.), xiii, 291; Sheet-flood erosion in Papague- ria, W. J. McGee (rev.), xviii, 228; Gypsum in, Blake, xviii, 394; An- thracite coal, W. P. Blake, xxl, 345; Remains of Bos, Wi PR: Blake, xxii, 65, 247; Distribution of metallic wealth (rev.), xxiii, 125; Remains of the mammoth, Blake, xxvi, 257; Salient features in its geology ;,W. P. Blake, xxvii, 160; Silicified trees, O. C. S. Car- ter (p.s.n.), xxvi, 259; Conglom- erate dykes, M. R. Campbell, PX ons Arkansas, Rep, Geol. Sur., 1887, Branner,. i, 65; Ozark uplift, Broadhead, iii, 6; Second Annual report, iii, 269; Resources (p.s.n.) iii, 279; Neocomian and chalk, Marcou, iv, 357; Neozoic geology, Hill; (rev.),; iv, 243; Bauxite, J. C. Bramnern Vil, 281s" ‘Geol, sur., (rev.), vii, 259, 263, 269; Coman- che series, R. T. Hill (rev.), viii, 259; Geol. Sur.,- (rev.), viii, 261, 329; Iron deposits, R. A. F. Pen- rose, (rev.);> x; 324: Report for 1891-2, Branner, (rev.), xiv, 394; Tertiary Geology, Harris (rev.), xiv, 394; Indurated Tertiary sandstone, Call (rev.), xiv, 395; Origin of novaculites, Griswold (rev.), xvi, 261; Red river and Clintan monoclines, Newsom and Branner, xx, 1; Batesville sand- stone, Weller, (rev.), xxi, 129; Geol. reports (p.s.n.), xxiii, 394; Igneous complex of magnet cove, sf S. Washington, (rev.), xxvii, 2. Arlington iron (meteoric), N. H. Winchell, xviii, 267. Armes, W. D., Autobiography of, Jos. Le Conte, (rev.), xxxii, 396. Arnheim beds,. Distribution of brachiopoda, A. F. Foerste, xxxvi, 244, Arnold, Ralph (p.s.n.), xxxii, 198; Marine Pliocene and Pleistocene of San Pedro (rev.), xxxiii, 49; (p.s.n.), SOOLEL, 396; (p.s.n.), xxxv, 324; Some crystalline rocks of the San Gabriel mountains, California (rev.), xxxv, 391. Arrangement and ey ores of plates in the Melonitidae (abs.), Jackson and Jaggar, xvi, 239. Arrowpoints from the Loess at Muscatine, Iowa, F. M. Witter, Ix, 276; Found with bones of Bison occidentalis in western Kansas, S. W. Williston, xxx, 313. Artesian wells, at Davenport, Tif- fany, iii, 117; at Woodhaven, L. I., Bryson, iii, 214; Stillwater, Minn., Meeds (p.s.n.), iil, 342; in South Dakota, Todd (cit.), Iv, 255; from the Archean (p.s.n.), Iv, 392; in Kansas, and cause of their flow, R. Hay, v, 296; at Keokuk, Volumes I-XXXVI. 7 with water power, A. §S. Tiffany (p.s.n.), Ws 128% from »the drift, C. W. Rolfe; vi, 32; in North and South Dakota, Upham, vi, 211; Government investigation (p.s. n.), vii, 271; between 97 degrees of longitude and the Rocky mountains, R. Hay (rev.), xi, 113; at Key West, Fla., E. O. Hovey, (abs.), xviii, "218; Hydraulic gra- dient in the Northwest, Als) 82 Todd (abs.) xviii, 219; of a por- tion of South Dakota, prelim- inary report, N. H. Darton (rev.) ix, 274; of Illinois, Leverett (rev.), xix, 418; in New Jersey and Long Island (rev.), L. Woolman, xx, 136; of Jowa, é (rev.), Xx, 2725, of Georgia, S. W. McCallie (rev. iF xxv. 251; of Tex- AS se bien. McLee. 384; at Min- Bee ats; N. H. Winchell, xxxv, 6 aS as an Archean term, Il, Asbestus and asbestiform minerals (abs.), G. P. Merrill, xvi, 240. Ashburner, C. A., Petroleum and Natural Gas in New York state @ev.) sp sil;—-430 obit) ave lass aa ead sketch, AS Winslow, vi Ashley, Geo. H., The Neocene strat- igraphy of the Santa Cruz moun- tains (rev.), xvii, 331; xxvli, 328; The Ditney folio, USS) G.'S.; (rev.); xxxi, 255, 283. Asia. Tectonic geography of east- ern, W. H. Hobbs, xxxiv, 69, 141, 214, Side Asiatic Russia, G. F: Wright (rev.), DO BPA Association of Western Naturalists, (p.s.n.), iii, 63 Association of Government Gecl- ogists, Proposed, viii, 196. Association of gastropod genus Cy- clora with phosphate of lime de- posits, A. M. Miller, xvil, 74; Ar- gillaceous rocks with quartz vee: O. A. Derby (rev.), xxiv, Associated minerals of rhodolite, Hidden & Pratt (rev.), xxlil, 328. Astronomical conditions favorable to glaciation, G. F. Becker (rev.) xiv, 191, Atlantic coast, Quaternary of. C. H. Hitchcock, fi, 300. Atlantic group of the Meyer, ii, 93. Atlantic Highlands section of the New Jersey Cretacic. J. K. Pra- ther, xxxvi, 162. Atwood, E. H. Movement of ice on Minnesota lakes, vii, 252. Atwood, W. W., Geology and Geog- raphy of the Devil's lake region and the Dalles of Wisconsin, (rev.) xxvi, 252. Atmospheric condensation a cause of solar heat. J. H. Kedzie (rey.), iv, 183. Attempt to explain glacial lunoid furrows, A. S. Packard. v. 104. Attitude of the eastern ana central portions of the United States during the Glacial period, T. C. Tertiary. (o/e) Chamberlin, viii, 288, 267. Augen-Gneiss area at Bedford, New York, Luquer and Ries, xviii, 239. Aughey, Samuel, Geyserite in Ne- braska. (cit.), i, 277. Augite syenite near Loon lake, New York (abs.), P. Cush- ing, xxiii, 106, 330 (rev.). Augusta, Use of the term in ge- ology, C. R. Keyes, xxi, 229 Auriferous gravels of the Sierra Nevada. H. W. Turner, xv, 371. Australasia, Ancient glaciation in. C. ‘H. Hitchcock, xxiii, 252; Mt. Lofty ranges, W. H. Howchin, (rev.), xxxv, 114. Australia, Evolution of, A. C. Greg- ory, (abs.), xvi, 114. Australian Tertiary mollusca, G. F._ Harris, (rev.), xxi, 383. Australian Institute of Mining En- gineers, (p.s.n.), xii, 6d. Autobiography of Jos. Le Conte, W. D. Armes, xxii, 396. Autodetus and some paramorphic shells of the Devonian, M. Clarkes sci, zit. Avalanche of ice on the Gemmi Pass, xvii, 359. Average elevation of the United States, Gannett, (rev.), xv, -62. Aviculipecten, typical species and generic characters, G. H. Girty, xxxili, 291, xxxiv, 3382; W, Hind, xxxiv, 200. Avi-fauna of the Silver lake region, Oregon, Shufeldt, vii, 235. Award of geological medals at Lon- don, viii, 62. , Awards in the department of Mines and Metallurgy, St. Louis Pur- chase Exposition, xxxv, 62, 130. Auxology, Terms of, Buckman and Bather, xii, 43; (ed. com.), xil, 257; A. Hyatt, xii, 290; (ed. com.), xii, 326. Azoic system and its subdivisions, P. Frazer, ii, 184; Definition of, (ed. com.), v, 106; Azoique terrain de Bretagne, fossils in, Barrois, (rev.), xi, 118. Aztecs, used meteoric iron, Hen- soldt, iv, 37; B Babcock, EF. G. (and F. A. Wilder), Geol. Sur. of North Dakota, sec- ond report, (rev.), xxxi, 383. Backbone of the continent, Wheeler, (p.s.n.), vii, 270. Backstrom, H., Causes of magmatic differentiation. (rev.) xiii, 194, Tvenne nyupptackta svenska klot- graniter, (rev)., xiv, 53; Vestina- faltet; En petrogenitisk studie, (rev.), xxi, 385, Backward step in paleobotany, G. F. Matthew, (rev.), xxIx, 251. Bacubirito meteorite of Mexico, H. A. Ward, xxx, 203; J. G. Agui- lera, (cit.), Bagg, R. M.. (p.s.n.), 131, 400; Oc- eurrence of Cretaceous fossils in The American Geologist. December, 19805. the Eocene of Maryland, xxii, 370; Cretaceous foraminifera in New Jersey, (rev.), xxiii, 126; (p.s.n.), xxxii, 61; Earthquakes in Socorro, New Mexico, xxxiv, 162; Foram- inifera of the bluff at Santa Bar- bara, Cal:, xxxv, 123. Bahamas, Expedition to, A. Agas- siz, (abs.), xiii, 141° Bailey, E. H. S., (cit.), v, 250; (p.s. Ts) axe. Bailey, G. E., (p.s.n.), iv, 254. Bailey, L. W., Explorations in New Brunswick, Quebec. and Maine, (rev.), v, 246; Relations between the geology of Maine and New Brunswick, (rev.), vi, 390; Geol- ogy of southwestern Nova Scotia, (pisin:.)), xX, 08> Jerogress, of sin= vestigations in southwestern Nova Scotia, -(rev.);, xiv; (605) .G@o:s-ne), xvi, 197; Bain, H. F., (p.s.n.), xii, 129; Pecul- iarities of the Mystic coal seam, xiii, 407; (p.s.n.), xv, 835; Central Iowa section of the Mississippian series, xv, 317; (and J. E. Todd,) Interloessial till near Sioux City, (rev.), xvi, 61; Preglacial eleva- tion of Iowa, (rev.), xvi, 62; (p.s. n.), xviii, 58, 265; Glacial drift in central Iowa, (rev.), xx, 272; Geol- ogy of Polk county, (rev.), Xx, 334; Drift in southwestern Min- nesota and northwestern Iowa, (abs)., xxi, 186; Aftonian and pre- Kansan deposits of southwestern Iowa, xxi, 255; (and A. F. Leon- ard), Middle coal measures of the western interior coal field, (abs.), xxiii, 251; Interglacial de- posits in Iowa, xxii, 3826; Notes on the drift of northwestern Iowa, xxiii, 168; (p.s.n.), xxiv, 66; (p.s. n.), xxvi, 63; Western interior coal field, (rev.), xxx, 124; (p.s. fy XO ae Le Gisele) ie eMC Ae, 394; (p.s.n.), xxxiii, 68, 202, 332; (peS.n.)y XX ees Baker, James, Annual report, mines oF tien Columbia, (rev.), xvil, 95. Baker, Marcus, cp.s.n.), xxl, 382; (p.s.n.), xxil, 129; (obit.), xxxill, 61. Balanus proteus, J. A. Cushman, xxxiv, 298. Baldwin, Judge C. C., (cit.), Opin- ion of Charles Whittlesey, iv, 267. Bald mountain, New York, Struc- eee according to Emmons, vil, Baldwin, S. Prentiss, Recent changes in Muir glacier, xi, 366; Pleistocene history of the Cham- plain valley, xiii, 170 Baldwin, W. J., (p.s.n. Ny, vill, 404. Ball, —, The cause of an ice age, (rey). sachs 202: Ball, R. S., ‘Wanderings of the north pole, (rev.), xil, 2. Ball, Valentine, (obit.), xvi, 203. Bather, A., Remarks on _ Golliez section in the geological hand- book of Switzerland, xv, 62. : Bandai are of Japan, Hobbs, xxxiv, 285, 291. Banded structure of some Tertiary Index, Volumes I-XXXVI. 9 gabbros, Geikie and Teall, (rev.), xv, 1238. Baoussé Roussé, New discoveries at, Nadaillac, x, 296. Baraboo iron ore, N. H. Winchell, XxXxXiv, 242. Bacnee Geology, Jukes-Browne, viii, 4 Barber, W. B., Lamprophyres and associated igneous rocks of the Rossland district, .xxxiii, 335, (obit.), xxxv, 399. Barbour, E. H., (and Torrey), Me- teorites of Iowa, viii, 65. Barbour, JE. 'H., “(p:s:n:).. viii, 64, 196; Nebraska geological survey, vol. 1, (rev.), xxxiii, Barite and selenite crystals in Mon- tana, J. P. Rowe, xxxiii, 198. Barlow, A. E., Huronian and Laur- entian contact north of lake Hu- ron, v, 19; Nickel and copper de- posits of Sudbury, Ont., (rev.), viii, 114; Relation of the Laur- entian and WHuronian north of lake Huron, (abs.), xi, 138; ditto, (reyv.), xiii, 63; Some dikes con- taining huronite, (p.s.n.), xv, 68; ditto, (rev.), xvi,! 119; (p.s:n.), xxix, 398. Barnacles from Gay Head, Mass., J. A. Cushman, xxxiv, 293; Paleo- zoic, structure of, J. M. Clarke, xvii, 137 : Barrande, Discovery of the primor- dial fauna in Britain, ii, 77; Opin- ion of the Taconic system, il, 77; And the Taconic system, Jules Marcou, iii, 118. Barrell, Jos., Physical effects of contact metamorphism, (rev.), PEM os! OC DsSli-)e XX, = aos Barrett, R, L., The Sundal drain- age system in central Norway, (rev.), xxvii, 1238. Barris, W. H., (obit.), xxvlill, 64; Sketch of his life, C. H. Preston, xxviil, 358. Barrois, Chas., The terms of the Cambrian, (p.s.n.), ii, 366; Granu- lites du Morbihan lil, 271; (cit.), Iv, 50; Correlation of pre-Cam- brian of Hurope and North America, (cit.), viii, 255; Sur la présence de fossiles dans le terrain azoique de Bretagne, (rev.), xl, 118; Rouvilligraptus richardson, (rev.),xii, 336; Des relations des mers Devoniennes de Bretagne et des Ardennes, (rev.), xxiii, 386; Extension du Silurien supérieur dans- le Pas de Calais, (rev.), xxiii, 386; Les Goniatites du ra- vin de Conlarie (rev.), xxiii, 386; Barrows, Franklin, Geological chap- ter of the Agassiz association, vill, 129. Barton, G. H., (p.s.n.), vl, 402; (p. s.n.), ix, 412; Channels in drum- lins, (rev.), xlii, 224; Former ex- tension of glaciation in Greenland and in Labrador xvill, 379; Gla- cial observations in the Umanak district, Greenland, (rev.), Xx, 329° (p:s.n.), xxvil, 397; (p:s.n.), xxvil, 327. Barus, Carl, Viscosity of solids (rev.), Ix, 342; (p.s.n.), xvi, 129. Basal complex, Neponset valley, Mass., W. O. Crospy, xxxvi, 3%; Beyond the southern end of tne Rocky mountains, C. R. Keyes, Xxxvi, 112, Basanite from Wyandotte (rev.), vii, 382. Bascom, Florence, (p,s.n.), xil, 69; Structures, origin and nomencla- ture of the acid volcanic rocks of South mountains, (rev.), XIII, 122; (p.s.n.), xv, 336; Serpentine and diabase, (abs.) xvii, 346; Re- lation of the streams in the neighborhood of Philadelphia to the Bryn Mawr gravels, xix, 50; Ancient volcanic rocks of South mountains, (rev.), xix, 139; Fin- land excursion of the 7th Int. Cong. Geologists, xx, 339; On some dikes in the vicinity of Johns bay, Maine, xxiii, 275; (p. s.n.), xxxiv, 401. Basal line of Carboniferous’ in northeastern Missouri, Keyes, x, 380. Bashore, H. B., Columbia deposits Ae the Susquehanna, (abs.), xvili, 8. Basic eruptive rocks in Androscog- gin county, Maine, G. P. Merrill, x, 49. Basic rock derived from granite, C. H. Smyth, Jr., (rev.), xiv, 199. Basic rocks of northeastern Mary- land, A. G. Leonard, xxvili, 1365. Basin range structure in the Death valley region of southeastern Cal- ifornia, M. R. Campbell, xxxl, OieLe Basins of the great lakes, origin of, J. W. Spencer, vii, 86; In gla- cial lake deltas, Fairchild, (avs), xxii, 254. Baskerville, 264. Bassler, R. S., (p.s.n.), xxxiii, 396. Bastin, E. C., A Permian glacial invasion, xxix, 169. Bath meeting of the British Asso- ciation (ed. com.), ii, 419. Bather, F, A., Museum arrange- ment, (p.s.n.), x, 260; (and Buck- man), Terms of auxology xii, 43; Crinoidea of Gotland, (rev.), xiil, 355; Brachiocrinus and Herpeto- erinus, xvi, 213; Wachsmuth and Springer’s monograph on crinoids, (rev.), xxiv, 56; What is an echi- noderm?, (rev.), xxviii, 257; Echi- cave Chas... (DiS) cl, noderma, (rev.), xxviii, 389. Batocrinus calvini, R. R. Rowley, v, 146. Batrachian and other footprints from the coal measures of Jog gins, G. F. Matthew, (rev.) xxxil, 54: Of eastern Canada, G. F. Matthew, (rev.), xxxv, 181. Bauer, L. A., Magnetic declination tables, and principal facts relat- ing to the earth’s magnetism, (rev.), xxxi, 123. Baur, G. Remarks on Dinosauria, (rev.), viii, 55; (p.s.n.), viii, 64; (p.s.n.), xxii, 180. i Bausch-Lamb petrographical micro- scope, G. H. Williams, (cit.), iil, 229. fe) Bauxite in Arkansas, J. C. Bran- ner, -vilj) Led: Bayley, W. S., Synopsis of Rosen- busch’s classification, (rev.), iil» 48; Peripheral phases of the gab- bro of Minnesota, (abs.), xv, 67; Summary of progress in mineral- ogy in 1894, (rev.), xv, 186; ditto in 1895 (rev.), xvii, 335; (and Van Hise), Preliminary report on the Marquette iron district, (rev.), xviii, 320; Progress of petrography The American Geologist. December, 1905. bearing Brachiopoda: devel- opment of Terebratalia obsoleta Dall, (rev.), xii, 188; Larval forms of trilobites from the lower Helderberg, (rev.), xii, 384; Devel- opment of the brachial supports in Dielasma and Zygospira, (rev.), xii, 394; On the mode of occur- rence and the structure and de- velopment of Triarthrus becki, xiii, 38; Further observations on the ventral structure of Triarth- in 1896, (rev.), xix, 350; -(p.s.n.), XK, 99s (lS: )) KV OnD- Beaches of lake Agassiz, (rev.), Warren Upham, i, 64; of Long Island, Bryson, ii, 64, 136; Nipis- sing VE Bai Laylorm. xv 5045) Jor lakes Warren and Algonquin, Up- ham, xvii, 400; Beach phenomena at Quaco, N. B., C. L. Whittle, vii, 183. Beachler, Chas. S., Keokuk at Crawfordsville, ii, 407; Crinoidea at St. Paul) Ind:, iv, 102; Rocks at St. Paul -Ind:, vii,.178: Rocks of Niagara age in Indiana, ix, 408; Keokuk group of the Miss- issippi valley, x, 88; Small pre- glacial basins in northwestern In-: diana, xii, 51; (obit.), xiii, £40. Beam, Wm., (and H. Leffmann), Examination of water for sanitary and technical purposes, iii, 334. Bearing of paleontological facts on nomenclature, H. S. Wollisme, rus, xv, 91; The larval stages of Trilobites, xvi, 166; Structure and appendages of Trinucleus, (rev.), xvi, 259; Sketch of James Dwight Dana, xvii, 1; Supposed discov- ery of antennae of trilobites by Linnaeus, in 1759, xvii, 303; On the validity of the family Bohe- millidae, xvii, 360; Occurrence of Silurian strata in the Big Horn mountains and in the Black Hills, xviii, 31; Systematic posi- tion of the trilobites, xx, 38; (p.s. Ma), XX, loss. WCDES a )s OCI elo aes Sketch of O. C. Marsh, xxiv, 185; Note on a new Xiphosuran from the upper Devonian of Pennsyl- vania, xxix, 144; Studies in evo- lution, (rev.), xxix, 182; (obit.), xxxiii, 189; Sketch of life and work of J. M. Clarke, xxxiv, 398. Beecherella, A new genus of Os- tracoda, E. O. Ulrich, viii, 197. Beede, (J: W.;- (p:S.n))5) XXvil; vosls (rev.), xxxvi, 49; ‘ Age of the Kansas-Oklahoma red Bearing of physiography on_uni- beds, xxviii, 46; Cottonwood Falls formitarianism, W. M. Davis, folio, (rev.), xxxiv, 262; (p.s.n.) (abs.), xvi, 243. aOR TL ‘Sollards Bear River formation. White and IY ee ene Sg Pome ee tratigraph h t- Stor denier seal? Stratigraphy of the eastern ou ia erop I Se ermian, Becke method of determining re- a ates POPES R12 fraction, W. O. Hotchkiss, xxxvi, Beginnings of American science, 305. Men feu é Goode, (rev.),’ ii, 429. Becker G. 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Williams, xv, 69; Cephalopod beginnings, xv, 125: On Nanno,° (cit.), xvi, 1; Structure of certain paleozoic barnacles, xvii, 137; James Hail ana the New York state survey, xviii, 55; A sphinctozoan calci- sponge from the upper Carbonif- erous of eastern Nebraska, Xx, 387: (p.s.n.), xxiii, 67; (and James Hall), Memoir on Dictyospongidae, (rev.), xxiv, 304; Upper Silurian fauna of the Rio Trombetas, Bra- zil, (rvev.), xxiv, 311; (and C. Schuchert), The nomenclature of the New York series of geological formations, xxv, 114; (p.s.n.), xxvi, 195: (p.s.n:), xxx, 130; An- notations of Jackel’s theses on Orthoceras and other cephalopods, xxxi, 216; (and R. Ruedemann). Guelph fauna in the state of New York, xxxii, 254; Naples fau- na in western New York. (rev.), xxxiii, 47: (p.s.n.), xxxiii, 397; Charles Emerson Beecher, xxxiv, DV Es(O 1S.) OGM, ere cite ele). D. Luther), Watkins and Elmira ousdrangies, (rev.), xxxiv, 324; Portage crinoids, (ed. com.), xxxv, 246; James Hali and the Troost manuscrivt, xxxv, p. 256. Clark, W. B., Tertiary of the Cape Fear river region, (rev.), v, 119; (and G. H. Williams). Geology of Maryland, (rev.). x, 63; Correla- tion paper. Eocene. (rev.), xli, 399: (and G. H. Williams), Geol- ogy and physical features. of Maryland, (rev.), xii, 396; Climate of Maryland. (rev), xiii. 139; Greensands of N. J., (rev.), xiii, 910: Mesozoic Echinodermata of the United States, (rev.). xiv. 329; Wocene fauna of the middle At- lantic slope. (rev.). xvi, 239; Eo- ecene deposits of the middle At- lantie slope, (rev.), xix, 64; Geol. Sur. Maryland, vol. i. (rev.), xxii, 875; Maryland geological survey, vol. ii, (rev.), xxiii, 193; ditto, vol. iii, (rev.), xxv, 383; Report on Allegany county, Md., (rev.), xxix, 119; Maryland geological survey, vol. iv, (rev.), xxxi. 54; Maryland geological survey, Mio- cene. (rev.), xxxv, 392. Classification of igneous’ rocks. Rosenbnusch’s,. Bayley’s scheme, (rev.). tii, 48; of the Cambrian and nre-Cambrian, R. ip Irving, (rev.). iv, 111: of eruptive rocks, Michel Levy. (rev.), iv, 308; of the chief geographic features of Tex- 24 The American Geologist. December, 1905. as; Re LT. Hill, -v,. 9) 68;) of Ameri- can paleozoic crinoids, S. A. Mil- ler, vi, 275; of the glacial sedi- ments of Maine, Geo. H. Stone, (rev.), vil, 186; of mountain ranges, Warren Upham, (rev.), Ix, 205; of the theories of the or- igin of iron ores, H. V. Winchell, x, 277; of the Cepholopoda (rev.), X, o2c; ditto, B.-A. Bather,” x, 396; of the Dyas, Trias and Jura in northwest Texas, Jules Mar- cou, x, 869; of the Brachiopoda, C. Schuchert, xi, 141; of topogra- phic forms, S. H. Perry, xii, 153; of economic geological depcsits, xili, 249; Rules and misrules in stratigraphic, J. Marcou, xix, 35; of costal forms, F. P. Gulliver, (abs.), xxii, 2538; Ice-contact of glacial deposits, J. B. Wood- worth, xxiii, 80; of igneous rocks, Lewinson-Lessing, xxiii, 346; of igneous rocks according to com- position, J. /.. Spurr xxv, 210; of igneous rocks, W. H. Hobbs, (rev.), xvii, 52; of the erystalline cements, E. C. Eckel, xxix, 146; Quantitative, of igneous rocks, (ed. com.), xxxii, p. 48; of sedi- mentary rocks, A. W. Grabau, xxxiii, 228; New, of Blastoidea, G. Hambach, (rev.), xxxiil, 45;. Ba- trachian foot-prints, G. F, Mat- thew, (rev.), xxxiii, 259; Upper Cretaceous of New Jersey, Stuart Weller, xxxv, 176. : Clay, what constitutes a clay, (ed. com.), xxx, 318. Clayey bands of the drift of the delta of the Cuyahoga river, and of the delta at Trenton, N. J., G EK. Wright, (rev.), xxii, 250. Clay and kaolin deposits of Hu- rope, H. Ries, (p.s.n.), xxi, 266. Clays, origin and distribution of Minnesota, C. P. Berkey, xxix, alae Clays and clay industry of Wiscon- sin, E. R. Buckley, (rev.), xxx, 329. ‘ Claypole, E. W., Darwin and geol- ogy, I, 152, 211; Subterranean commotion near Akron, Ohio, |, 199; The future of natural gas, I, 31; Lake-age in Ohio, (rev.), I, 63; Condition of the interior of the earth, i, 382; (p-s.n.), 396; Earthquake tremors at Charles- ton, S. C., li, 185; Clark’s collec- tion of fishes at Borea, Ii, 62; Glaciers and glacial radiants in the ice age, iii, 73; Vascular na- ture of the trees of the Coal Meas- ures, fii, 55; The story of the Mississippi-Missouri, iil, 361; (cit.), iv, 337; Illustration of the ‘Yevel of no strain’? in the crust of the earth, v, 83; Making of Pennsylvania, v, 225; Paleontolo- gical notes from Indianapolis, vl, 255; Notice of the death of Frank- lin C. Hill, vii, 68; Megalonyx in Holmes Co., Ohio, vil, 122, 149; Episode in the paleozoic history of Pennsylvania, viii, 152; Pre- Glacial channel near Akron, Ohio, (abs.), viii, 195; Deep boring near Akron, (abs.), viii, 239; Geologic correlation, (abs.), viii, 251; New fishes from the Cleveland shale, (abs.), ix, 217; The tin islands of the northwest, ix, 228; (p.s.n.), Ix, 282; Gigantic placoderm from Ohio, x, 1; Geology of the British association at Edinburgh, x, 188; Dentition of Titanichthys and its allies, (p.s.n.), x, 193; The head of Dinichthys, x, 199; A new coc- costean, Coccosteus cuyahogae, xi, 167; Pre-Glacial man not im- probable, xi, 191; Cladodont sharks of the Cleveland shale, xl, 325; The three great fossil placo- derms of Ohio, xii, 89; On Glypto- dendron in Ohio, (cit.), xii, 133; Early man in America, (abs.), xl, 175; Three new species of Dini- chthys, xii, 275; A new species of Carcinosoma, xiii, 77; Cladodus, a new selachian, xiv, 137; A new placoderm from the Cleveland shale, xiv, 379; On a new speci- men of Cladodus clarki, xv, 1; Recent contributions to our knowledge of the cladodont sharks, xv, 363; (p.s.n.), xvl, 129, 328; Actinophorus clarki, xvi, 20; Glacial notes from the planet Mars, xvi, 91; Geology at the British association for the ad- vancement of science, xvi, 300; The time piece of geology, xvii, 40; A new Titanichthys, xvii, 166; Ancestry of the upper Devonian placoderms of Ohio, xvii, 349; Dinichthys prentis-clarki, xviii, 199: Ancient and modern sharks, and the evolution of the class, (abs.), xviii, 222; Human relies in the drift of Ohio, xviii, 302; A new Dinichthys—Dinichthys kep- leri, xix, 322; International con- gress of geologists, xx, 203; (p.s. n.), xx, 420; Paleozoic geography of the eastern United States, (abs.), xx, 200; Paleolith and neo- lith, xxi, 3838; Microscopical light in geological darkness, xxii, 217; Glacial theories—cosmical and terrestrial, xxii, 310; The earth- quake of San Jacinto, Dec. 25, 1899, xxv, 106, 192; (p.s.n.), xxv, 129; Notes on petroleum in Cali- fornia, xxvii, 150; (p.s.n.), xxvil, 130; (obit.), xxviii, 247; Bio- graphical sketches, by Comstock, Richardson and Bridge, xxix, 30; Bibliography, xxix, 40; (p.s.n.), xxx, 71; The Devonian era in the Rae basin, xxxii, 15, 79, 240, 312, CiayeeD stone axe, (p.s.n.), xxxl, Cleavage, different structures de- seribed under, Van Hise, (p.s.n.), xvii, 125; Discussion by Geo, F. Becker, (p.s.n.), xvli, 126. Clements, J. M., Some stages in the development of rivers, (abs.), xvii, 126; Study of some exam- ples of rock variation, (rev.), xxii, 381; Contribution to the study of contact metamorphism, (rev.), XXIV, 54 (andes da. snrych)s Crystal Falls iron-bearing district Index, Volumes I-XXXVI. of Michigan, (rev.), xxiv, 308; et: KeVi 195: (p:S-n.)), xxxill, 62, t Clendenin, W. W., (p.s.n.), | xill, 133; (p.s.n.), xv, 130; Preliminary report on the Florida parishes of east Louisiana and the bluff, prairie and hill lands of south- west Louisiana, (rev.), xviii, 322. Cleveland water supply tunnel, S. J. Pierce, xxviii, 380. Cliffwood clays and the Matawan, G. N. Knapp, xxxiii, 23; ditto, E. W. Berry, xxxiv, 253. Climatic changes indicated by the glaciers of North America, I. C. Russell, ix, 322. Climatic conditions shown by North American inter-glacial de- posits, Upham, xv, 273; ditto, G. M. Dawson, xvi, 65. Clinton iron ore, Origin of, C. H. Smyth, Jsx., (rev.), x, 122. Clinoplains of the Rio Grande, C. L. Herrick, xxxiii, 376. Close of the twentieth volume, (ed._ com.), xx, 403. Clypeastridae, A new Cretaceous genus of, F. W. Cragin, xv, 90. Coal, anthracite, valley of the Bow river, Jas. A. Dodge, 1, 172; Cas- cade anthracite basin, Geo. M. Dawson, i, 332. Coal, anthracite, exhaustion of, (ed. com.), iil, 45. Coal and metal miner’s book, (rev.), xxviii, 126. Coal deposits of Iowa, C. R. Keyes, (rev.), xiii, 353. Coal field of southeastern Ken- tucky, Crandall and Hodge, (rev.), i, 65; of Cinnabar and Bozeman, Montana, (rev.), viii, 54; of Mis- souri, A. Winslow, (rev.), xi, 271; Cerillos of New Mexico, J. J. Stevenson, (rev.), xvii, 94; Around Tsé Chou, China, N. F. Drake, (rev.), xxxiii, 260; Western in|te- rior, H. F. Bain, (rev.), xxx, 124; of Montana, J. P. Rowe, xxxii, 3609) or Alaska, -(pis-n:), xxxiv, 401; Bituminous of Pennsylvania, Ohio and West. Virginia, I. C. White, (rev.), ix. 264; foundland, J. P. Howley, (p.s.n.), Vai 20. Coal formation, Side light upon, W. S. Gresley, xiii, 69. Coal in Colorado, A. Lakes. (rev.). v, 312; in the south of England, (DSi) ALVie Oloee Cannelse from Kootanie, D. P. Penhallow, x, 331; of Crow’s Nest pass, Selwyn, (abs.), xi, 181: Anthracite in Ari-’ zona, W. P. Blake, xxi, 345: spe- cial report on Kansas coal. E. Haworth, (rev.), xxii, 384; In low- pocket er Michigan, (p.s:n.). xxv, 59; on: Turkey creek, Colorado. (p. s.n.), xxxli, 132; in Spitzbergen, J. J. Stevenson. (abs.), xxxv, 192. Coal and plant-besring beds of Australia and Tasmania, Feist- mantel, (rev.), vi, 320. Coal plants. vascular nature of the tree, E. W. Claynole. fii. 55; Pos- sible new, W. S. Gresley, xxlv, 199; ditto, xxvi, 49; ditto, xxvil, of sNew=-= | 25 6; of the Coal Measures of Missou- ri, D. White, (rev.), xxvi, 55; of Indian territory, D. White, (rev.), xxvi, 58 Coal Measures, chert in Iowa, (ed. com.), i, 116; Fossils from the lower at Des Moines, C. R. Keyes, ii, 285 Sof eentral’= lowar C.* R. Keyes, ii, 396; Fauna of the low- er, C. R. Keyes, (rev.), ii, 432; Vascular nature of trees in, E. W. Claypole, iii, 55; of Indian ter- ritory, H. M. Chance, vi, 238; Lower of Monongalia and Preston counties, W. Va., S. B. Brown, Ix, 224; A new fungus, Herzer, xi, 365; Unconformity with the St. Louis, C. R. Keyes, xii, 99; Dac- tyloporus archaeus, MHerzer, xii, 289; Unio-like shells in Nova Scotia, Whiteaves, (rev.), xiii, 193; of Blount mountain, Gibson, (rev.), xiii, 284; of Big Stone gap, M. R. Campbell, (rev.), xiv, 392; New _ trilobite from Arkansas, A. W. Vodges, (rev.), xvi, 262: of western interior coal field, H. F. Bain, (and. A. TT. Leonard), (abs.), xxii, 251; Horizon in New Mexico, Herrick and Bendrat, xxv, 234; of Kansas, C. R. Keyes, XXV;5 (3475 “Bireclays’ of, Vio GC Hopkins, xxviii, 47; in Arizona, E. T. Dumble, xxx, 270; Bryozoa, Nebraska, G. E. Condra. xxx, Baits Erratic boulder in Tennessee, S. W. McCallie, xxxi, 46; Footprints in the Joggins, G. F. Matthew, (rev.), xxxii, 54. Coal mining in Pennsylvania, (p.s. M15) XVII SOO: Coals of Colorado, J. S. Newberry, (rev.), ii, 429. Coal mines in China, and in British Columbia, (p.s.n.), iii, 62. seat oy at Florence, Colo., (p.s.n.), ii, 62. Coarseness_ of igneous rocks and is meaning, A. C. Lane, xxxv, oO. Cohen, E., Meteoritenkunde, (rey.), XV, 328. Coast ranges of California, pre- Cretaceous rocks of, H. W. Fair- banks, xi, 69; Notes on the geol- ogy of, Turner and Stanton, xlv, 92; Contribution to the geology, AS (C2 Mawson, xv, 342%" Coast ranges, age of, F. L. Ransome, xix, 66. Cole, Granville, A. J., (p.s.n.), xvii, 257. Coleman, J. P., Inter-glacial fos- sils from the Don valley, xlll, 85; Geology of the Rocky moun- tains between Saskatchewan and Athabasea, xiv, 83; Rainy Lake fold region, (rev.), xvi, 313; The Iroquois beach at Toronto and its fossils, (rev.), xxiii, 103; The Huronian question. xxix, 325; Duration of the Toron?o inter- glacial epoch, xxix, 71. Collecting fossils in the Cincin- ley shales, H. E. Dickhout, xxiil, 335. Collenot, J. J., (obit.), xi, 363. . 20 The American Geologist. Collet, John, (obit.), xxiii, 338. Collie, G. L., Geology of Conanicut island, R. Ey (rev.), xv, 386; Ori- gin of conglomerates, (rev. Ne xvii, 126. Collier, A. J., (p.s.n.), xxxiv, 67. Colorado, Geology and mining in- dustry of Leadville, S. F. Em- mons, (rev.), i, 194; Coals of, J. S. Newberry, (rev.), ii, 429; Coal oil at Florence, (p.s.n.), iii, 62; Mesozoie of southern, J. J. Stev- enson,, iii, 391; Extinct volcanoes, A. Lakes, v, 38; Ore deposits, A. Lakes, (rev.), v, 57; Coal deposits, A. Lakes, (rev.), v, 312; Fossil but- terflies of Florissant, S. H. Scud- der, (rev.), vi, 197; Geology and physiography of northwestern, Cc. A. White, (rev.), vii, 57; Fish remains in lower Silurian, C,. D. Walcott, (p.s.n.), vii, 208; ditto, (ed. com.), vii, 329: Fuel resour- GesxwAs Lakes, viii, 7; Supposed Trenton fish, (ed. com.), viii, 178; Spherulitic crystallization, Cross and Iddings, (vd. com.), viii, 387; Llama remains, FE. W. Cragin, ix, 257. Peculiar schists near Salida, Cross) (ew) xine i20E Geology and western ore deposits, an Lakes, (rev.), xii, 261; Sandstone dikes in granite, Cross, (abs.), xiii, 215; New Liriodendron from the Laramie, Hollick, | (p-s.n.)) xiv, 203; Erosion interval be- tween Tertiary and Quaterna- TY Guba) Canmon, Cp Sa.) Sex 406; New Cretaceous genus of Clypeastridae, F. W. Cragin, xv, 90; Fossil fishes of Canyon City, (ed: com.), xv, 121; Natural gas at Manitou, Wm._ Striebly, (rev.), xvi, 116; Post-Laramie deposits, (rév.),, xvi, 120; Cripple. Creek gold mining district, J. F. Kemp, (abs.), xvii, 193; Uranite,, Pearce, (rev.), xvii, 396; Lacco- litic locality, G. K. Gil- bert and W. Cross, (abs.),. xvil, 407; Underground water in Ar- kansas valley, G. K. Gilbert, (rev.), xix, 57; Sandstone dikes of the Ute pass, Crosby, (p.s.n.), xx, 68; Tourmaline and tourma- line schists, H. B. Patton, (rev.), xxii, 251; Arechean-Potsdam con- tact, W. ©O.:Crosby, (rev.), xxiii, 92; Geolog gy of the Aspen mining district, J. BE. Spurr, (rev.), xxiv, 307; Tellurides from, Cc Palache, (rev.), xxvii, 181; Thomsonite, mesolite and chabazite from Gold- en, H. B. Patton, (rev.), xxvii, 183; Carnotite and associated vanadiferous minerals, Hillebrand and Ransome, (rev.), xxvii, 185; Granitie rocks of the Pike’s peak quadrangle, E. 3B. Matthews, (rev.), xxvii, 254; Areal geology of the Castle Rock region, W. py Ween xxix, 1966 Cladodus from the Devonian, O! Pa slay, 373; Ore devosits in all forma- tions, xxxi, 326; Coal on Turkey ereek, (p.s.n.), xxxii, 182; Hang- ing valleys of Georgetown, W. O. Crosby, xxxii, 42; Geology of western ore deposits, A. Lakés, XXX, December, 1905. (rev.), xxxvi, 319. Colorado turmation and its inverte- brate fauna, T. W. Stanton, (rev.)), Teiv, 1, Colorado river of Texas, geologi- cal history, R:. T. Hill, iit, 28% Colorado Scientific Society, (p.s.n.), xvi, 68. Color of soils of high and low lat- itudes, W. O. Crosby, viii, 72. Color Sets Int. “Cong. «Geol: iy oO. Colossal cavern, Kentucky, H. C. Hovey; (abs.), xviii, 228; Bridges of Utah, (ed. com.), xxxiv,. 189. Columbian exposition, (ed. com.), geological maps at, xii, 250; Ex- hibit of petroleum, xii, 323; Ex- hibits in the mines and mining building, xii, 376; Additional mod- els, W. M. Davis, xii, 340; (ed. com.), Gems, native metals and other rare minerals, xiii, 415; Harvard university geological ex- hibit, xiii, 279; Pleistocene geol- ogy, xiii, 109; Mesozoic and Ter~ tiary exhibits, xiii, 185; ditto, T. W. Stanton, xiii, 289; Mineralogy and petrography, Ga. ish Williams, xiii, 345; Ores of the noble and useful metals, (ed. com.), xiii, 48; Vertebrate paleontolog y; John Eyerman, xiii, 47. Columbia formation, McGee, (rev.), ii, 130; Distribution on the At- lantic slope, N. H. Darton, (abs.), xi, 244; in northwestern Illinois, (OW MET ‘Hershey, (abs.), xiv, 203; ditto, O. H. Hershey, xv, 7. Columbia university, summer school, H. W. Shimer, xxx, 69; (p.s.n.), xxx, 202, 271, 336; Fall excursions, H. W. Shimer, xxxi, 62; Summer field work, H. W. Shimer, xxxil, 130% “Cpisin)y poet, 197; 5259: Comanche formation, (Am. Com.), lis 268s4iv, 3s5%5 Of; the! Pexas-—Ar- kansas region, R. Ef. Hill, (ev.); viii, 259; the Mentor beds, a Com- anche terrane in central Kansas, Em W, Cragin, xvi, 162. Comatula from the Florida reefs, F. Springer, xxx, 98. Commemorative tablet: of the American Association for the Ad- vancement of Science, (ed. com.), xxix, 178. Common zeolites of the Minnesota shore of lake Superior, N. H. Winchell, xxiii, 176. Composite generic fundamenta, Ae M. Clarke, xiii, 286. compa of Eozoon, (ed. com.), x5 Comparative taxonomy of the rocks of the lake Superior region, N. H. Winchell, xvi, 331. Comparison of Pleistocene and pres- ent ice sheets, Upham, (rev.), xl 29: Complete geography, supplement by W. M. Davis on New England, (rev.), xvii, .328. Comstock, F. M., Wave-formed cusp at lake George, N. Y., xxv’ 192; Small esker in western, N. ies Xxxii, 12; Ancient lake beaches in Georgian bay, xxxiii, 312. Index, Volumes I-XXXVI. 27 Comstock, Theo. B., Mineral re- sources of Arkansas, (rev.), Iii) 2g apes ive) 253° (p.s.n.), Vili, 196; E. W. Claypole, the scientist, xxi 1: : Conanicut island, R. I., Geology of, G. LL. Collie, (rev.), xv, 386. Concannon farm, Pleistocene geol- ogy, N. H. Winchell, xxxi, 263. Concho county, Geological survey of, Cummins and Lerch, v, 321. Concrete examples of topography from Howard Co., Iowa., S. Cal- Vill XX, GD, Concretions in the Chemung of southern New York, HE. M. Kin- dle, xxxiii, 360. Condensation and conflagration the- ories of the suns heat, J. H. Ked- zie, (rev.), iv, 182, 183. Conditions of accumulation of drumlins, Upham, x, 339; of ero- ston beneath deep glaciers, N. S. Shaler, (rev.), xii, 191; of ripple- mark formation, T. A. Jaggar, Jr., xiii, 199; and effects of the ex- pulsion of gases from the inte- rior of the earth, N. S. Shaler, (abs.), xvi, 244. Condon, Thos., Two islands and et came of them, (rey.), xxxvi, Condra, G. E., New Bryozoa from the Coal Measures of Nebraska, xx, 337; on Rhombopora lepido- dendroides, (Meek), xxxi, 22; an gld Platte channel, xxxi, 361; (p. $.n.), xxxiv, 67. Cone in cone in the Devonian in Pennsylvania, W. S. Gresley, (rev.), xiv, 399. Confounding of Nassa trivittata and N, peralta, G. D. Harris, viii, 174. Conglomerates in gneissic terranes, A. Winchell, iii, 153, 256; in New England gneisses, C. H. Hitch- cock, iii, 253; Dikes in southern Sg M. R. Campbell, xxxill, D. Congress. Int, of Geol., P. Frazer, i, 8. 86; Proceedings of, the Paris meeting, i, 6: of the Bologne meeting, 1, 87; of the Berlin meeting, i,: 93; Nomenclature adonvted for rock masses, etc., l, 90; for species. i, 91; Color scheme for maps. i, 97; London meeting, reports of the American commit- tee, ii, 139; ditto, iii, 343; P. Fra- zer, iv, 44; Philadelphia meeting, Frazer, v, 208; Berlin meeting, report of, (rev.), ii, 431; (ps-n.), xii, 131; Reviews of the Ice-age at the World’s Congress on Geol- DEN. mieXlbs, precio SOLttOs moxlt yer: Int. Cong. Geol., St. Pet- ersburg meeting. (ed. com.), xix, 344; xxi, 123; Finland excursion, F. Bascom. xx, 339: Eighth ses- sion), (Paris); BP. BPrazer, _xxvil, 835; Ninth session, xxxiii, 61. Connecticut, Triassic in the Con- necticut valley. W. M. Davis, (rev.), iv, 112: Fishes and plants of the Triassic, J. S. Newberry, (rev.), iv, 187; Two belts of fos- siliferous black shale in the Triassic, Davis and Loper, (rev.), viii, 118; Ice sheet on Newton- 7 ville sand plain, F. P. Gulliver, (abs.), xii, 177; Eastern boundary of, the Triassic, W. M. Davis, (abs.), xiii, 145; Quarries in the lava beds, W. M. Davis, (rev.), xvii, 189; Physical geography, W. M. Davis, (rev.); xvii, 250; Quartz vein near Mystic, J. F. Kemp, (abs.), xviii, 63; Triassic tufl-beds and pitchstone, B. K. Emerson, (abs.), xviii, 220; Thames river, fDi any oe Gul- liver, (rev.), xxiii, 104; Granites on the north share of Long Island sound, J. F. Kemp, (rev.), xxiii, 105; Granites of southern Rhode Island and Con- necticut, J. F. Kemp, (rev.), xxv, 122; ditto, (rev.), xxvii, 51; Gran- ite-gneiss area in central, L. G. Westgate, (rev.), xxvii, 121; New footprint from the Connecticut yaney, J.° AS” (Cushman; -Socddhit, Conrad’s Tertiary fossils, proposed reprint, (p-s.n.), xi, 282; Dall’s collection of Conrad’s works, G. D. Harris, xi, 279; Republication by G. D. Harris, (rev.), xii, 60. Considerations sur les fossiles de- erits comme Algues, G.’ Maillard, (rev.), ii, 54. Consolidation of the American Geologist with Economic Geology, (ed. com.), xxxvi, 309 Contact of the Laurentian and Huronian north of lake Huron, A. E. Barlow, vi, 19; Metamorphism of the Palisades diabase, J. D. Ir- ving, (p.s.n.), xxi, 398; Phenom- ena of the Palisade diabase, J. D. Irving, (rev.), xxvii, 53; Metamor- phism of a basic igneous rock, Us. Se Grant. (rev): 9 xvi ow; Physical effects of contact meta- morphism, J. Barrell, (rev.), xxix; Sis. Continental area of the Devonian, (Am, Com.), ii. 232; Divide in Nicaragua, C. W. Hayes, (rev.), xxii, 253. Continental glacier, effect of pres- sure. A. Winchell, i, 139. Continental problems. G. K. Gil- bert, xii, 118; Continuity of the Glacial period, Dr. Holst on, G. F. Wright, xvi, 398. Contributions to the paleontology of Brazil, C. A. White, (rev.), I 257: to micropaleontology, E. Ulrich, (rev.), v. 107; to Canadian paleontology. J. F. Whiteaves, (rev.), v, 108; to the geology of the southwest, R. T. Hill, vii, 119, 254: to invertebrate paleon- tology, R. P. Whitfield. (rev.), vii, 882: to the geology of the great vilains, Robt. Hay, (rev.), xi, 56; to the invertebrate paleontology of the Cretaceous of Texas, (rev.), xfil, 124; (cit.), xili, 289; to the knowledge of the pre-Glacial drainage of Ohio, W. G. Tight, (rev.), xiv, 188: to the minera- logy of Wisconsin, W. H. Hobbs, (rev.), xvi. 263: to the Cretaceous _naleoantology of the Pacific coast, T. W. Stanton, (rev.), xix, 63; 8 The American Geologist. December. 1905, & letude des terrains sedimen- taires, (rev.), xxii, 388; to the study of contact metamorphism, J. M. Clements, (rev.), XxiVv, 254; to the geology of Fox river ‘valley, S. Weidman, (rev.), xxiv, 257; to the geology of the north- ern Black hills, J. D. Irving, (rev.), xxvi, 322; to the geology of Maine, H. S. Williams and H. E. Gregory, (rev.), xxvii, 256; to the Tertiary fauna of Florida, W. HH. Dally sev Ux 218; (obit.), xix, 364; Sketch by Helen D. King, xxiii, 1; Life and letters, P. Frazer, xxvi, 67; Cata- logue of his publications, 1859- 1897, P. Frazer, (rev.), xxxi, 180. Copper-bearing rocks, Name of, U. S. Grant, xv, 192. Copper deposition, Theory of. A. C. Lane, xxxiv, 297; Handbook HB. J. Stevens (rev.), xxxvi, 187. Copper deposits in Canada, R. Bell, (rev.), vii. 261. Copper in the Animikie rocks, A. C. Lawson. v. 174: In the iron “ mines at Soudan. Minn., (p.s.n.), xxi, 382; Native in Oklahoma, E. Haworth, (p.s.n.). xxvi, 195. Copper minerals. Note on certain,” A. N. Winchell. xxviii, 244. Cooper mines of Rio Tinto, Spain, James Douglas, (abs.), xxix, 192. Corals described by D. D. Owen in 1838, S. Calvin, xii, 108. Corals and coral islands, J. D. Da- na. (rev.), vii, f Coral formations, Darwin's theory, i, 212; Murray’s theory, i, 113, 213; Some new contributions to the discussion, (ed. com.) lncoale Hicks, L. E., The reef builders, (p.s.n.), vii, 389. Cordierite and its associates, Nat- uray HiStoryaol ee eam Teall, (rev.), xxv, 384. Cordilleran geological club, (p.s.n.), Malis 7o" : Cordillera and Laurentide glacia- tion, R. Chalmers, vi, 324 Cordilleran paleozoic sea and its specimcnts C. D. Walcott, xil, 57 Cornell college, Iowa, Dept. of Ge- ology, (p.s,n.), xxiv, 391. Cornell summer school of field ge- ology, C. E. Smith, xxx, 396. Ccrrelation of the Lower Silurian, EH. O. Ulrich, i, 100, 179, 303; Dit- to, ii, 39; Of the stages of the Ice age in North America and Europe, Warren Upham, xvi, 100. Correlation of Warren beaches with moraines and outlets in south~ western Michigan, F. B. Tay- lor. (ADS. a xXVilige 2oereOLaainiO= raines with beaches on the bor- der of Lake Erie, F. Leverett, xxi. 195; In the Ozark region: a correction, O. H. Hershey, xxiv, 190; Of the sub-divisions of the Coal Measures of Kansas, C. R. Keyes, xxv, 347. Correlation: Orotaxis a method of, C, R. Keyes, xviii, 289. Correlation papers: Devonian and Carboniferous, H. S. Williams, (rev.) eo1x,. bs) \Cambriany ia ps Walcott. (rev.). ix, 203; Creta- GCenuss Cus Ade Wehites (reve) ips 121s oOo LOCENE, m aVVermMles Clark, (rev.), xii, 399; Neocene, Dall and Harris, (rev.), xii, 399; Newark system, I. C. Russell, (rev.). xii, 402; Cretaceous, A. White (rev.), xii, 119. Corundum in North Carolina, J. H. Pratt, (rev.). xxvi, 393. Coste, Eugene, Mines and mineral statistics of Canada for 1887, (rev.), v. 247. Cote sans dissein and Grand Tow- er. Cache Marbuty pc 86. Coville—F V.. (o.sm-.). xvil. 3846. Coxe: E. B., (obit.); ‘xvi, 66. Cragin, F. W., New _ or little known saurian from Kansas, il, 404; Cheyenne sandstone of Kan- Sas, Viz 233 ivils 3289 79 \(pessn)) vii, 270; On a leaf-bearing ter- rane in the Loup Fork, viii, 29; (v.s.n.), viii, 68; Observations on the genus Trinacromerum, viil, LiL (pisses. Xilpmeatee Contripu= tion to the invertebrate paleon- tology of the Texas Cretaceous, (rev.), xiii, 124; New fossils of the Neocomian of Kansas, xiv. 1; A new Cretaceous genus of Cly- peastridae, xv, 90; The Mentone Index, beds, a central Kansas terrane of the Comanche series, xvi, 162; A study of the- Belvidere beds, xvi, 357; The plains Permian, xvili, 131; Observations on the Cimarron series, xix, 351. Crandall, A. R., Whitely and Pu- ore counties, Ky., (rev), vil, Crandall and Hodge, Coal fields of southeastern Kentucky, (rev.), i; 65. crater lake, Oregon, (p.s.n.), xviii, Crane, Agnes, Generic evolution of paleozoic brachiopods, xi, 400; Evolution of the Brachiopoda (rev.), xiii, 194. Crawford, J., Geciogical survey of Nicaragua, vi, 377; Recent earth- quakes in Nicaragua, vii, 77; Neo- lithic man in Nicaragua, vili, 160; The Viejo range of Nicaragua, viil, 190; Evidence of a Glacial epoch in Nicaragua, viii, 306; Notes on earthquakes in Nica- ragua, x, 115; Recent severe seis- mic disturbances in Nicaragua, xxii, 56; Decrease of water in lake Nicaragua, xxvi, 257; Heavy rains and possible voleanic action in Nicaragua, xxviii, 328; Earth- quakes in Nicaragua, xxix, 323, 3938; List of the most important voleanic eruptions and _ earth- quakes in western Nicaragua within historic time, xxx, 111, 395; Rignon de la Viejo, xxx, 130. Crawford, J. J., (p.s.n.), xvil, 59. Gredner, H., (cit.), viii, 241, 246; (p.s.n), xvi, 327. Cresson, H. T., and the Delaware river dwellings, S. D. Peet, v, 190. Cretacic in America, (Am. Com.), ii. 259, 263: Foraminiferal origin of, R. T. Hill, iv, 174; Discovery of mammals in, in Wyoming and Dakota, O. C. Marsh, (rev.), iv, 109; Discovery of the Ceratopsi- dae by Prof. Marsh, (rev.), v, 181. Cretaceous and Tertiary of Ser- gipe-Alagoas basin of Brazil, J. C. Branner, (rev.), vii. 121. Cretaceous of Texas, R. T. Hill, vi, 252: Pitot Knob. Texas. marine voleano, R. T. Hill, vi, 286; Near Wilmington, N. C., T. W. Stan- ton, vii, 333; Of California and Oregon, G. F. Becker, (rev.) vil, 258; Covering of the Palezoic in Texas. Ss) Parry ix, 169s. OF Mexico, Heilprin, (rev.), x, 121; Laramie, The close of the Cre- taceous, Cross, (rev.). x. 256; Of Iowa and the sub-divisions of Meek and Hayden, xi, 300; Of northern California and Oregon, dS: Diller, “(eev,), xil, 119; Cor- relation paper, C. A. White (rev.), x, 121, xii, 119; Of northern Min- nesota, H. V. Winchell, xii, 220; Fossil plants from Min- nesota. Lesquereux, (rev,). xil, 330; Fossils collected by James Fector in British N. America, in 1857-60. J. F. Whiteaves. (abs.), xiv. 68: New genus of Clypeas- tridae, F. W. Cragin, xv, 90; Fos- t Volumes I-XXXVI. 29 sil plants from Minnesota, L. Les- quereux, (rev.), xv, 384; Plants from Martha’s Vineyard, A. Hol- lieck,;- @ev-); --XViz- 2095 9 Mossil sponges in the flint nodules of the Lower Cretaceous, J. A, Merrill, (rev), XVilbeipes Olaye Marke ‘at Cliffwood, N. J., A. Hollick, (abs.), xviii, 230; Paleontology of the Pacific coast, T. W. Stanton, xix, 68; Coast ranges, Age of, F. Ransome, xix, 66; Clay and marl at Cliffwood, N. J., xx, 137; Cre- taceous fossils in the Eocene of Maryland, R. M. Bagg, Jr, xxii» 370; Age of the Amboy clay se- ries, as indicated by its flora, A. Hollick, (abs.), xxil, 255; Fora- minifera of New Jersey, R. M. Bagg, Jr., (rev.), xxiii, 126; Low- er, of Kansas, C. N. Gould, xxv, 10S) Of Texas, Re JD Veal rev): xxx, 384; In Greece and Crete, L. Cayeux, xxxi, 386. Crete, Jurassic and Cretaceous, L. Cayeux, (rev.), xxxi, 386. Crinoidea, modifications in classi- fication, Wachsmuth and Spring- er, (rev.), iii, 200; From the Ni- agara Limestone, C. S. Beachler, iv, 102; Republication of Lower Carboniferous, Whitfield, (rev.), xiii, 124. Crinoids, Structure of Crotalocrin- us, Wachsmuth and Springer, (rev.), iii, 201; Batocrinus cal- vini, R. R. Rowley, v, 146; Agari- cocrinus, C. H. Gordon, v, 257; Of the Niagara at Lockport, N, Y., E. N. S. Ringueberg, (rev.), vi, 250; Work of Wachsmuth and Springer, (p.s.n.), i, 132; Summit plates of blastoids, erinoids and cystids, Wachsmuth and Spring- er, (rev.), i, 61; New genus, S. A; Miller, i, 263; Natural casts from the Burlington, R. R. Row- ley, vi, 66; Structure, classifica- tion and arrangement into fam- ilies, S. A. Miller, vi, 275, 340; Perisomic plates, Wachsmuth and Springer, (rev.), vii, 225; Criti- cism of S. A. Miller, vii, 272; Re- ply of P. H. Carpenter, vii, 386; Head of, Dyche, x, 130; Reproduc- tion of arms, A. F. Foerste, xil, 270, 340; From Missouri, Rowley, xii, 803; Of Gothland, (rev.), xIil, 855; And brachiopods from Mis-~ souri Hamilton, xiii, 151; Amer- ican, Wachsmuth and Springer, (p.s.n.), xiv, 407; Bracheocrinus and WHerpetocrinus, Bather, xvl, 218; Wachsmuth and Springer’s monograph (rey.), xxiv, 56; New Cystocrinoidean, F. W. Sardeson, xxiv, 263; From Missouri, R. R. Rowley, xxv, 65; Development of Agaricocrinus. Mary Klem, (rev.), XXXVI» 1607 sores: 7 in. fistulate crinoids, F. Springer, xxvi, 133; New discovery concerning Uinta- crinus, F. ‘Springer, xxiv, 92; From Missouri, Rowley, xxv, 67; Further note on Uintacrinus, F. Springer, xxvi, 194; Pores in the ventral sac of fistulate crinoids, 38 F. A. Bather, xxvi, 307; Structure and relations of Uintacrinus, Wrank springer, (rev.), xxviii, 258; Actimnemetra from the s#lor- ida reeis, H. Springer, XXX, Yd; Sagenocrinus and forbesiccrinus, F. springer, xxx, 838; New Cys- toidea and a new Camarocririus, C. Schuchert, xxxii, 280; With re- gard to Portage (ed. com.), xxxv, 246, Crincids and blastoids; R. R. Row- ley, rev.), vili, 186; Blastoids and eystoids from Missouri, KR. kK. howley, XxXv, 65. Criteria of subglacial and engiacial drift, Warren Upham, viil, 376. Criticai notice of the stratigraphy of the Missouri paleozoic, Broad- head, xii, 74; Periods in the his- tory of the Earth, J. LeConte, CEE XVI, woln Croil ,James, on pre-nebular con- ditions; 7 (cits), av. 20; (obit., p.s.n.), vii, 207. Croll’s Theory redivivus, (ed. com), xxvii, 174. . Crook, A. R., Geological causes of the scenery of the Yellowstone park, xx, 159; Biographical sketch of Oliver Marcy,. xxiv, 67. Cozzens, issachar, Jr., Biographical sketch, A, W. Vogdes, xxiv, 327. Crosby, W. O. ‘Tables for the de- teriuination of minerals, (rev.), fi, 340; Finer portions of the till, (p.s.n.), Vv; 1235. Color ‘of ‘soils’ of high and low latitudes, viii, 72; Origin of parallel and intersect- ing joints, xii, 369; Geology of the Boston basin, (rev.), xii, 192; (cit.), xiii, 205; Origin of pegma- tites, (rev.), xiii, 215; Tables for the determination of minerals, (rev.), xvi, 262; Sea mills of Ce- phalonia, xvii, 265; Englacial drift xvii, 203; Glacial lakes of the Boston basin, (p.s.n.), xvii, 128; (with M. L, Fuller), Origin of pegmatite, xix, 147; Sandstone dikes of the Ute pass, (p.s.n.), xx, 68; History of the Blue Hills complex, Boston basin, (abs.), xxii, 268; Glacial lake of the Nashua valley, (rev.), xxiii, 102; Archean-Potsdam contact in the vicinity of Manitou, Col., xxiii, 92; On the origin of phenocrysts and development of the porphyr- itic structure, xxv, 299; Geologic- al history of the Nashua valley, (rev.), XXV; 252; p.S.n.), xxvi, 398: Geology of the Boston basin, vol. i, part iii, (rev.), xxvii, 179; are the amygdaloidal melaphyrs of the Boston basin intrusive or contemporaneous? xxvii, 324: Ori- gin of eskers, xxx, 1; Hanging valleys of Georgetown, Col., xxxii, 42; (p.s.n.),) xxxil, 197, 332; Dene- ous rocks of the lower Neponset, Mass., xxxvi, 34, 69. Cross-banding of strata by current Action. J. B. Woodworth, xxvii. 281. The American Geologist. December, 1905. Crossing the Valdez glacier at Bates pass, W. R. Abercrombie, xxiv, 349. Crosskey, H. W., (obit.), xiii, 75. Cross, VW/hitman, Close of the Cre- taceous, (rev.), x, 256; Peculiar schists near Salida, Colo., (rev.), xi, 120; Sandstone dikes, (abs.), xiil, 215; Diorite of the Ophir loop, (abs.), xvii, 345; (p.s.n.), xvii, 408; (p.s.n.), xxxiii, 64. Crucial points in the geology of the lake Superior region. N.. H. Win- chell, xv, 158, 229, 295, 356; Ditto, xvi, 12, 75, 150, 205, 269, 331. Crustacea, Bibliography of Paleu- zoic, 1698-1889, A. W. Vogdes, (rev.), vii, 379. Crystal Falls iron-bearing district of Michigan, Clements and Smyth, (rev.), xxiv, 308. Crystalline rock near the surface in Pawnee county, Neb., F. W. Rus- Sell, 124305 Crystalline rocks later than the Ar- ehen, (Am. Com.), ii, 164; Crys- talline schists, (p.s.n.), il, 367; Recent work on, by Prof. Judd, (Gdkss Comis)pa salwar alain Rocks of southern California, O. H. Her- shey, xxix, 273; Of the San Ga- briel mountains, Arnold and Strong, xxxv, 391; Rocks of Mis- souri,, BD. Haworth, (rev.), ix, 750. Crystall!ne schists, relation to secu- lar rock decay, R. Pumpelly, (rev.), vil, 259. Crystalline limestones, ophiolites and associated schists of the east- ern Adirondacks, J. F. Kemp, (abs.), xv, 61. : Crystallization. Spherulitic, (ed. com.), viii, 387. Crystallized slags, from copper smelting, A. C. Lane, (abs.), xv Crystallogenesis, H. Hensvoldt, v, 3801, 375. Crystallography: A treatise on the morphology of crystals, N. Story- Maskelyne, (rev.), xvil, 538; Ble- ments of, Moses and Parsons, (rey.). xxvl, 328; Elements of, G. H. Williams, (rev.), ix, 208. Crystals. Characters of, A. J. Mos- es, (rev.), xxili, 389. Cuba, Mineral resources, lL. E. Levy. (rev.), xxlil. 328; Harriet C. Brown, (rev.). xxxii, 187; Sun- posed union with Florida. Re- joinder to Dr. Dall’s criticism. J. W.. Spencer, xxxiv, 110. Cuhanite et Rutte. Ment., Winchell, xxii, 245. Culver, G. &. Plans for irrigation in. Dakota, (pis-n.), iv, 389; A fit- tle Known region in northwestern Montana, (rev.), xi, 412; The ero- sive action of ice, (rev.), xvi, 316. Cumings: “Es Ro) (piss), -xxibe 74: Orthothetes minutus, n. sp., from the Salem limestone of Harrods- burg. Ind.. xxvii, 147; Revision of certain bryozoan genera, xxix, H. V. ~—— Index, Volumes I-XXXVI. 31 ISepes.n), xxxii; s3l:: (and €. S. Prosser), Waverly fromations of Central Ohio, xxxiv, 335; De- velopment of Fenestella, xxxv, 50. Cummins, W. F., Carboniferous in Texas, (p.s.n.), ii, 138; On the Concho country, v, 321; New Car- boniferous coral, Hadrophyllum aplatus, (rev.), viii, 187; (and E. T. Dumble), The Double mountain section, ix, 347; Report on The Texas survey, (rev.), x. 311; Tu- eumcari mountain, xi, 375; On Cerro Tucumeari (cit.), xii, 103; (and E. T. Dumble), The Kent section and Gryphaea tucumceari, xii, 309; A question of priority, xv, 395. Curtice,’ Cooper, Oriskany drift near Washington, iii, 223. Curtis, Geo. C., West Indian erup- tions of 1902, xxxi, 40; Relief of the earth’s surface, xxxii, 178. Cushing, F. L., (cit.), xvi, 255. Cushing, H. P., Notes on the Muir glacier, Alaska, viii, 207;° Mr. Cushing on the Muir glacier, G. F. Wright, viii, 330; (and Weins- ehenck), Zur genauen Kentniss der Phonolithe des Hegaus, (rev.) xi, 274; The faults of Chazy township, Clinton county, (abs.), xv, 66; Areal geology of Glacier bay, Alaska, (abs.),- xvii, 61; Dit- to, (rev.), xvii, 331, Are there pre-Cambrian and _ post-Ordovi- cian trap dikes in the Adiron- dacks? (abs.), xvii, 407; Ditto, H. P. Cushing; (rev.), xviii, 390; Note on hypersthene-andesite from mount Edgecumbe, Alaska, xx, 156; Syenite-porphyry dikes in the northern Adirondacks, (rev.), xxii, 382; The boundary of the Potsdam north of the Adiron- dacks, (rev_.), xxiii, 330; Angite- syenite north of Loon lake, New York, (rev.), xxiii, 106, 330; Deri- vation of the rock name anortho- site, xxix, 190; Geology of Rand hill, N. Y., (rev.). xxix. 58; Geol- logical work in Franklin and St. Lawrence counties, N. Y., (rev.), Kee SNe Iuittle’ “Falls,, .N: Y., (rev.), xxxv, 250. Cushman. J. A., New footprint from the Connecticut’ valley, xxxiii, 154; Pleistocene forminife- ra from Panama, xxxiii, 265; Mio- ecene barnacles from Gayhead, xxxiv, 293; Fossils from Sankaty head, Nantucket, xxxv, 194. Cuspate forelands, F. P. Gulliver, (abs.), xvii, 98. oyrad: A new, T. H. M’Bride, xii, Cycles of sedimentation, J. L. Wil- liams, viii, 315. Cyclosphaeroma trilohatum, iste Woodward, (rev.). vii. 196. Czyszkowski. S.. Depnesition of gold in South Africa. (Translated by H. V. Winchell), xvii, 306. D Daimonelix, Remarks on, J. F. James, XV, 337; or Wat? ,éu. com.), xvi, 1138; J. F. James, Xvi.i, 198; Cast of burrow of rodent, Peterson, (p.s.n.), xxxiv, 268. Dakota formation (Am. Com.), li, 2638. Dakctas, Artesian water, prelimi- nary report, INS. HS “Darton, (rev.), xix, 274. Dakota Tin Mines, (p.s.n.), vi, 402. waie, T. Nelscn, The Greylock syn- clinorium, viii, 1; Rensselaer Grit plateau, (rev.), xiv, 54; (with Pumpelly and Wolff), Geology of the Green mountains in Massa- chusetts, (rev.), xvi, 386; Struc- tural details in the Green moun- tains, (rev.), xvili, 390; (p.s.n.), xxvii, 327; Structural details in the Green mountains and in east- ern New York (rev.), xxxi, 58, Dale, W. F., (p.s.n.), xvi, 67. Dall, W. H., Classification of the Tertiary. (Am. Com.), ii, 282; Peace Creek beds (rev.), vii, 382; Collection of Conrads works, G. D. Harris, xi, 279; Marine Mio- cene shells from Okhotsk sea, (p.s.n.), xii, 342; (and G. D. Har- ris), Correlation paper, Miocene, (rev.), xii, 399; Appalachicola river, Dall and: Brown, (rev.), xiii, 1837; Notes on the Atlantic Miocene, (abs.), xiv, 202; Contri- butions to the Tertiary fauna of Florida (rev.), xxvii, 179; Struc- ture of Diamond head, Oahu, XKVIi SOs sGWsSeke by) KOC heroes Contributions to the Tertiary of Florida, (rev.), xxxiii, 49; Ditto, C Sechuchert, xxxiii, 143; Spen- ecer’s rejoinder to Dall’s criticism of the hypothesis of the Union of Cuba and Florida, xxxiv, 110; Harriman expedition (rev.), xxxiv. 122. Dalles of the Wisconsin (p.s.n.), xxxiii, 396. Daly, R. A. (p.s.n.), xx, 180; (ps. n.), xxiii, 206: (p.s.n.), xxv, 393; (p.s.n.), xxvii, 129; Calecareous concretions of Kettle point (rev.), xxvii, 253; Physiography of Acadia, (rev.), xxvii, 316; (p. Sinby DoCVvill,. dode (pis. xOKis 194; N. E. coast of Labrador, Crave ye xexcix.) A256 o GDiS a) Cae 806: Variolitic pillow lava from Newfoundland. xxxii, 65: ("s.n ), xxxii, 332" (p.s.n.),.. secxtli> 60: Secondary origin of certain granites, (rev.), xxxvi, 312. Dana. E S., System of Miner?logy, 6th edition. (rev.), x, 64; Textbook (rev.), xxii, 328. Dana, James D.. Views on the Ta- conic, i, 165; Darwin’s theory of coral reefs, i, 300; (cit.), on Ta- conic. ii. 69; Nomenclature cf Lower Paleozoic (Am, Com), Il. 198: Characteristics of volcanoes. (rev.), vi, 194; Definition of Ta- 32 The American Geologist. December; 1905. conic mountains (cit.), vi, 247; Corals and coral islands (rev.), vii, 57; Walker prize, S. Hen- shaw ix, 409; (obit.), xv, 336; Manual of Geology (rev.), Xv, 259; (p.s,n.), Proposed memorial, xvi, 129; Biographical sketch, C. EH. Beecher, xvii, 1. Danbyborough, YVt., Camptonite dikes; VE: Masters, Xv, 368. Danzig, E., Eruptive nature of the gneisses and granites of the Mit- telgebirge (rev.), iii, 151. - Darton, N. H., A jointed earth au- ger, vii, 117; Mesozoic and Ceno- zoic of Virginia and Maryland, (rev.), viii, 185; Fossils: in the Lafayette formation in Virginia, ix, 181; Guide to Baltimore, (rev.) ix, 210; Traps of the New- ark in New- Jersey, (rev.), | ix, 260; Record of N. A. geology, 1887-89, (rev.), ix, 342; Central Appalachian in Virginia, x, 10; Distribution of the Columbia for- mation (abs.), xi, 134, 244; Cen- ozoic history of eastern Virginia and Maryland, (abs.), xii, 171; Green Pond to Skunnemunk, (rev.), xiii, 211; Faults between the Mohawk and the Adiron- dacks (abs.), xiv, 198; —(p.s.n.), xv, 67, 68; Coastal plain series (rev.), xvi, 288; Stratigraphic resumé (rev:), xvi, 238; Lower Coastal plain series, (abs.), xvii, 107; Resumé (abs.), xvii» 108; Stream robbing in the Catskills, (abs.), xvii, 98; Geology of the Black hills (abs.), xvii, 264; Ar- tesian water of the Dakotas, pre- liminary report, (rev.), xix, 274; Developments in well boring and irrigation in South Dakota, (rev.) xxi, 325; Fossil fish in the Jurassic of the Black hills (abs.), xxiii, 93; Mesozoic stratigraphy in s. w. Black hills (abs.), xxiil, 94; Shore line of Tertiary lakes, (abs.), SX VL e(and enna Clarke). On a hydromica from New Jersey (rev.), xxiv, 182; (p. Spee XXVil; Sos; (pIs.ny), x ) Buller; (abs.), viii, 239. De Geer, Gerard, Pleistocene changes of level in eastern N. America, xi, 22. De Lapparent (p.s.n.), ii, 367, 369. Delaware valley, Older drift, R. D. Salisbury, xi, 360; water gap, Em- ma Walter (rev.), xvi, 200, Eo- cene deposits of the Atlantic (rev.), xix, slope, W. B. Clark, 64 Del Castillo, Antonio, (p.s.n.), xvl, 328; (obit.),xvi, 400. De l’existence de Spongiaires dans le pre-Cambrien de Bretagne Cayeux, (rev.), xvi, 59. Delgado, |. F., Record of the Lon- don Int. Cong. Geol., iv, 44; (p. s.n.), v, 209; Fauna of Haut- Alemtejo (rev.), xxxiv, 192. Deltas of the Mohawk. F. B. Tay- lor, Ix, 344; Ditto, Warren Up- ham, ix, 410. Delta plain at Andover, Mass., F: S. Mills, xxxil, 162. Deming, J. L. (Herrick and E. S. Clarke). American norytes and gabbros, I, 339. K Denison University, Bulletins of the scientific laboratories (ed. com.), i, 117; Barney Memorial Hall burned (p.s.n.), xxxv, 261. Denton, F. W. (p.s.n.), xv, 272; (p. aby > td awl? A Department of geology, University of Nebraska, (p.s.n.), lil, 341; In the National Museum (ed. com.), xxviii, 107. Departure of the ice sheet from the Laurentian lakes, W. Upham, (abs.), xiv, 199. Devosition of gold in South Afriea. Czyscezkowski, xvii, 310. 34 The American Geologist. Derby, Orville A. Nepheline rocks in Brazil (rev.), i, 209; (p.s.n.), vi, 68; Nepheline rocks in brazil, (rev.), x, 326; Quartz veins in ar- gillaceous rocks (rev.), XXIV, 182; Mode of occurrence of topaz, (rev.), xxvii, 185. : Derivation of the rock name anor- thosyte, H. P. Cushing, xxix, 190. : ; Descloiseaux, A. (obit.), xxi, 332. Description of eight new Cambro- Silurian fossils from Manitoba, J. FE. Whiteaves, (rev.), Zo aot New crinoids, blastoids and brachiopods, R. R. Rowley, xii, 903: de quelques trilobites de 1] Urdovicien, bergerou, eves, Xv, 262; New fossils from Missouri, R. R. Rowley, xvi, 217; of Java and Madoura, Verbeek and Fe- Menia (lev.), XxX, 331; New LuSsiss from Missouri, R. R. Rowley, xxv, 261, Of new species of Clad- odus from the Devonian of Col- orado, O. P, Hay, xxx, 373. Desor, E., Laurentian as a Quater- nary term, (cit.), v. 33. ; Determination of common muner- als, W. O. Crosby, (rev.), xvi, 217; of feldspars by the methods of Michel Levy, G. F. Becker (p. s.n.), xix, 223; Of the feldspars. N. H. Winchell, xxi, 12; Of the Cambrian age of the Cambrian limestones of Missouri, C. R. Keyes, xxix, 384; Of the feldspars in this section, J. E. Spurr, xxxl, 376. Determinative mineralogy, Brush and Penfield, (rev.). xviil, 391. Development of some Silurian Brachiopoda, Beecher and Clarke, (rev.), v, 54; Of the corallum in Favosites forbesi var occidentalis, G. H. Girty, xv, 131; of rivers, illustrated by Deer river in Mich- igan, J. M. Clements, (abs.), xvil, 126: and growth of Diplograptus, R. Ruedemann, (rev.), XX, 136; of well boring and irrigation in South Dakota, N. H. Darton, (rev.), xxi, 325; Development of the Ohio river, W. G. Tight, (abs.), xxii, 252; and morphology of Fenestella, E.R. Cumings, (abs.), xxxv, 50. Devonian, Origin of the name, (Am. Com.), ii, 225; Areas in. North America, (Am. Com.),~ ii, 228; Continental area, (Am. Com.), ii, 232: Base of, (Am. Com.), ii, 237: Top of, (Am. Com.), ii, 239% Distinct marine faunas, (Am. com.), ii, 240; Not sharply divid- ed, (Am, Com.), ii, 242; Unsettled problems, (Am. com.), ii, 245; Faunas of Iowa, S. Calvin. iil, PASI faunas of Iowa, H. S. Williams, iii, 230; Remarks on the report of the American committee, J. Mar- cou, iii, 60; Plants from Ohio, J. S. Newberry, (rev.), v, 184; Plants from Scotland, (rev.), vi, 56: Thickness of in New York, December, 1905. C. S. Prosser, vi, 199; Middle De- vonian of western Australia, Nicholson and Hind, (rev.), vl, 322; Fossil fishes, (p.s.n.), vii, 143; Of Buchanan county, Iowa, Calvin, viii, 142; Correlation pa- per; SS Walliams;,. (rev) 58; Chemung and Catskill, J, J. Stevenson, ix, 6; Fish fauna of In Ohio and Germany, C. Ro- minger, xX, 56; Fauna of Altai Tschernyschew, (rev.),' xii, 335; Autodetus and paramorphic shells, J. M. Clarke, xiii, 327; Versteinerungen in brazil, Am- mon, (rev.), xiii, 427; Paleo- zoic fauna of the Ural Tscherny- schew, (rev.), xiv, 119; of eastern Pennsylvania and New York, C. S. Prosser, (rev.), xv, 262; Upper middle Devonian in the moun- tains of the Rhine, Holzapfel, (rev.), xvi, 389; Series in. S. W. Missouri,, Hershey, xvi, 294; Fish remains in Bohemia, Roenen, (rev.), xvi, 318; Formations of the southern Appalachian, C. W. Hayes, (abs.), xvii, 107; Discov- ery of new fish fauna, Mixer, xviii, 223; of the Rhine, Beushau- sen, (rev.), xviii, 124: the south- ern formations, H. S. Williams, (rev.), xx, 133; of Bretagne and Ardennes, C. Barrois, (rev.), xxiil, 386; Mollusks from Brazil, J. M. Clarke, (rev.), xxiv, 311; System in Canada, J. F. Whiteaves, xxiv, 210; Fish remains from the Hifel, Huene, (rev.), xxv, 251, 391; Lam- prey, Bashford Dean, (rev.), xxvi, 60; New Cladodus from Colorado, © QUP) Hay; Xxx; (33; Byravine the Ohio basin, E. W. Claypole, xxxil, 15. 79, 240, 312, 385; Paleontology, Williams and Kindle, (rev.), xxxvi, 49. Devonic of America and Russia, C. Schuchert, xxxii, 137. Dewalque, Prof. G., The Cambrian Silurian, Taconic, (p.s.n.), ii, 365; (cit.), v, 381; Use of the Taconic, (cit.), vlii, 184. le. pre-Cambrien de Cayeux, (rev.), xvi, 59. Diabase dikes of the Rainy lake region, “Ay C..lawson, ioe ei the Missouri Archean, HE. Ha- worth, i, 287. Dlabasic schists of northeastern Minnesota, H. V. Winchell, iii, 18. Diagonal moraine, F. G. Plummer, xi, 230), Diagram of barrier reef at Tahiti, ee Ehiecks sit) 30! Dlamonds, in meteorites, (p.s.n.), 1, 137; In Wisconsin, (p.s.n.), vil, 72; Second largest, (p.s.n.), x, 398; In meteoric stones, (p.s.n.), xl, 282; At the Columbian Exposition, Geo. H. Williams, xiii, 349; Ditto, (ed. com.), xiil, 416; In meteorites Huntington, (rev.) xiii, 254; in Bretagne, Index, Volumes I-XXXVI. 35 Wisconsin and their probable source, W. H. Hobbs, xiv, 31; In meteorites, Huntington, (rev.), xvi, 316; Genesis and matrix, Lewis, Bonney, (rev.), xx, 57; In California, H. Turner, xxiii, 182; From New South Wales, (p.s.n.), xxix, 129; The largest ever found, (p.s.n.), xxxv, 192. Diamond mines of South Africa, (ed. com.), xxxi, 51. Diatomaceous earth (pissn.), i; 136. Diceratherium in the White River beds of South Dakota, Wit ote Hatcher, xiii, 360; D. proavitum, pened tse Eoteher, xx, dls. Dickhaut, H. E., Collecting fossils in the Cincinnati shales, xxiii, 335. Dictionary of the fossils of Pennsyl- vania, Lesley, (rev.), v. 53; Ditto, (rev.), vii, 382; of altitudes in the United States, Gannett, (rev.), ix, 342; of altitudes of Missouri, C. F. Marbut, (rev.), xvii, 54; of alti- tudes in the United States, H. Gannett, (rev.), xxv, 121; Dictyonema cavernosum, (rev.), xx, 189. Dictyonema fauna of the slate belt, Ruedemann, (rev.), xxxiv, 55. Dictyospongidae, Hall and Clarke, (vev.), xxiv, 304 Didymograptus, ete. Ger. Holm, (rev.), xvi; ‘58. Dielasma, brachial supports, Beech.- er and Schuchert, (rev.), xii, 394. Die Beane eiszeit, Waagen, (rev.), il, 336. Diener, Carl, (cit.), viii, 242, 247. Differentiation, causes of magnetic, PAckstrém, (rev.), xiii, 194; Rela- tions among igneous rocks, Id- dings, (rev.), xiii, 195; Extrusive and intrusive rocks as evidences of magmatic, J. P. Iddings, (rev,), xx, 132: Of magmas, (ed. com.), xxii, 113; In rocks of the copper- bearing series, (abs.), xxii, 251; In m2gmas, Lewinson-Lessing, xxiii, 346. Differential We. Let) ElobpS; xiv, 35. Differences in batholitie granite ac- cording to depth of erosion (abs.), B. K. Emerson, xxiii, 104; _ Difficulties in deep coal mining, P. Turner, (abs.), xxviii, 334. Dikes near Kennebunkport,’ Me., J. F. Kemp, v, 129; Near Mt. Lyon, Clinton Co., N. Y., A. S. BHakle, xii, 31; Of Oligocene sandstone in the Neocomian clays, A. P. Pav- low, (rev.), xvii, 251; In the Adi- rondacks, H. P. Cushing, (abs.), xvii, 407; In the vicinity of Port- land, Maine, E. C. E. Lord, xxil, 335; Of felsophyre and basalt in Central Appalachian Virginia (rev.), xxiii, 327; In the vicinity of John’s bay, Maine, F. Bascom, xxiii, 275. Diller, J. S., Lavas of northern Cali- in Nebraska, Wiman, faults, fornia, (rev.); 1; 125; Volcanic dust, ii, 64; Sandstone dikes in Calitornia, (abs.), v, 121; Lassen Peak vdistrict, v(mevaan vise 196; (p.s.n., Taylorville region), ix, 215; Late voleanic eruption in N. California, (rev.), ix, 265; Taylor- ville region of California, (rey.), x, 183; The Cretaceous and Ter- tiary of the Pacific states, (abs.), xi, 139; Geol, soc. of Wash., xi, 281; Cretaceous and early Ter- tiary of northern California and Oregon, (rev.), xii, 119; Shasta- Chico series, (abs.), xiii, 208; Revolution in the topography of the Pacific coast since the aurif- erous period, (rev.), xiii, 354; (p.s.n.), xvi, 66; (p.s.n.), xviii, 60, 61; Hornblende basalt in northern California, xix, 253; Ori- gin of Paleotrochis, (rev.), xxiv, 182; (p.s.n.), xxix, 128; Topogra- Phic development of the Klamath mountains, (rey), ocean: (p.s.n.), xxxiii, 59; Dimetian, as a term in the Archean, (Am. Com.), ii, 163; Diminution of natural com.), viii, 176. Dinichthys, Head, E. W. Claypole, gas, (ed. XC LOSS ACClis) ey Pl eae Melani pole, (CLES Sct 94; Three new species, Claypole, xii, 275; Anatomy of, Bashford Dean, (rev.), xiii, 357; Ventral armor, A. A. Wright, xiv, 313; Prentis- clarki,. E. W. Claypole, xviil, 199; Dorsal shields, Cc R. Eastman, (abs.), RVI, eco. Column, fins and armor- ing, Bashford Dean, (rev.), xvili, 316; D. kepleri, Claypole, xix, 322. D’Invilliers, Phosphate beds of Na- vassa, (rev.), vil, 202; Certain eoantles in Pennsylvania, (rev.), Aube Sait Dinosauria, Remarks on, DY iG Baur, (rev.), viil, 55. Citney folio, Fuller and Ashley, (rev.), xxxi. 255. Diphyphyllum semacoénse, new characters, W. H. Sherzer, iv, 93. Dip!acodon beds (Am. com.), ii, 289. Diplograptus pristis, Development and growth, Ruedemann, (rev.), xx, 136. Directions for collecting and pre- serving fossils, C. Schuchert, (rev.), xvi, 262. Direction of pre-Glacial stream flow in central New. York, (ed. com.), xxxiil, 43; Ditto, Frank Carney, xxxill, 196. Discovery of the antennae of trilo- bites by Linnaeus in 1759, C. E. Beecher, xvii, 303; of a_ sessile Conularia, R. Ruedemann, xviil, 65; New fish fauna in the Devoni- an, F. K. Mixer, (abs.), xvill, 223; Fish in the Jurassic in the Black hills, (abs.), N. H. Darton, The American Geologist. Deeembertignes xxiii, 93; of the Laramie in Ne- braska, C. A. Fisher, xxx, 315; Of ais gas in Findlay, O., (p.s.n.), B Wee Discrimination of glacial accumula- tion and invasion, Warren Up- ham, (abs.), xv, 200. Discussion of the terms rock- weathering, serpentinization, and hydrometamorphism, G. P. Mer- rill, xxiv, 244. Disintegration of diabase at Med- set G. P. Merrill, (abs.), xvil, 91. Dislocations of the earth’s erust, Margerie and Hein, (rev.), II, 348; Tertiary of the Atlantic coast, N. S. Shaler, (abs.), xiil, 143; In the Atlantic plain and their causes, A. Hollick, (abs.), xiv, 197; Dismal swamp district, Virginia, N. S. Shaler, (rev.), ix, 206. Dissection of the Ural mountains, F, P. Gulliver, (abs.), xxii, 23. Disseminated lead ores of south- eastern Missouri, A. Winslow, (rev.), xix, 68. Distribution of certain Loess fossils, Cc. R. Keyes, iv, 119; Of stone im- plements in the tide-water coun- try, W. H: Holmes, (rev.), xi, 208; Of earthquakes in the United States, N. S. Shaler, (rev.), xiv, 396; Of land and fresh water mollusks of the West Indian re- gion, C. T. Simpson, (rev.), xv, 261; Of iron oxide, I. J. Wistar, (abs.), xvii, 261; Of Cambrian and Silurian in Siberia, Baron Toll, (rev.), xix, 1388; Of vanadi- um and molybdenum in the United States, Hillebrand, (rev.), xxii, 880; Of metallic wealth in Arizona, W. “Ps Blakes (rev); xxiii, 125; Of brachiopoda in the Arnheim beds, A. F. Foerste, xxxvi, 244; District of Columbia, Oriskany drift, Cooper Curtice, iii, 223. Diuturnal theory of the earth, Wm. Andrews, (rev.), xxv, 50. Diversity of the glacial drift, War- ren Upham, (abs.), xiii, 223. Divisions of the Ice age in the Unit- ed States and Canada, C. H. Hitcheock, xv, 330. Divining rod, Mechanical action of, M. E. Wadsworth, xxi, 72; Dodge, James A., Anthracite coal, Bow river, i, 172; (and N. H. Winchell), Kiowa meteorite, v, 309; Ditto, vi, 370. Codge, R. E., River terraces (rev.), xiv, 397; (p.s.n.), xvii, 2638; Pene- plains of eastern Tennessee, (abs.), xvii, 264; Scientific geog- raphy in education, (abs.), xxl, 201; (p.s.n.), xxvi, 259; New York Academy of Sciences, xxviii, 329; Ditto, xxix, 127; Ditto, xxix. 320; Elementary geography, (rev.), xxxiv, 197; Advanced geography, (rev.), xXxxv, 181. Dolomytes of eastern Iowa, N. Knight, xxxiv, 64. Don river in southeastern Russia, (rev.), xXxxiv, 121. Dorpat university, (p.s.n.), xii, 131. Doremus, C. A., (p.S.n.), XX, 68. Dotsero volcano, Colorado, Arthur Lakes, v, 40. Double Mountain section, Dumble and Cummins, ix, 347. Douglas, James, Famous copper mines of Spain, (abs.), xxix, 192; (p.s.n.), xxxiii, 395. Dowling, D. B., Red Lake, Be- rens river, (rev.), xvili, 389. Dragons of the air, H. G. Seeley, (rev.), xxviii, 323; Drainage systems of New Mexico, R. S. Tarr, v. 261; Of the Carbon- iferous area of Michigan, E. H. Mudge, xiv, 301; Modifications and their interpretation, M. R. Camp- bell, (abs.), xvii, 98; Trellised in the Adirondacks. Brigham, xxl, 219; Peculiarity in Androscoggin county, Maine, H. T. Burr, xxiv, 369; Features of southern cen- tral New York, (abs.), xxxv, 52. Drake, Ns F:, 7 (p:S.n.))), xocimealoas Coal fields around Tse Chou, Chi- na, (rev.), xxviii, 260; Prane colliery, Pa., (p.s.n.). iif, 215. Drayson, Gen., Cause of Glacial periods, (p.s.n.), xi, 63. Dresser. J. A., Petrography of Mt. Orford, xxvii, 14; of Shefford Mt., xxviii, 203. Drift deposits, a part of the Pleis- tocene. (Am. com.),. ii, 296; Of Long Island, J. Bryson, xxii, 245. Drift of the North German low- lands, R. D. Salisbury, ix, 294; Deposits of Germany, J. Bryson, x, 132; Succession of parts, R. Bell, (abs.), xi, 174; Englacial, Warren Upham, xii, 36; In S. W. Minnesota, N.-W. Iowa, H. F. Bain, (abs.), xxi, 136; Of north- western Iowa, H. F. Bain, xxiil, 168; In the Dakotas, Warren Up- ham, xxxiv, 151. Driftless area of the upper Missis- sippi, Chamberlin and Salisbury, (rev.), 4, 122. Drift mounds near Olympia, Wash., G. O. Rogers, xi, 393; Ditto, Bry- son, xii, 127; Ditto, Upham, xxxiv, By Drumlins, Structure of, W. Upham, (rev.), v, 61; Conditions of accu- mulation, W. Upham, (abs.). xX, 218: Ditto, x, 339; Osar kame for- mation, T. C. Chamberlin, (rev.), xii, 122; Madison type, Upham, (abs.), xiil, 222; Channels on, eaused by glacial streams. G. H. Barton, (abs.), xiii, 224; Origin of, R. S. Tarr, xiii. 393; Accumula- tion, Warren Upham, xv. 194; And marginal moraines of ice sheets, Upham, (abs.), xvi, 237; Index, Volumes I-XXXVI. 37 Containing or lying on modified E drift, Warren Upham, xx, 383; In the English lake district, xxi, 165; Eagle, Gov. Jas. P., On the Arkan- In Glasgow, Upham, xxi, 285; Ar- | nas "survey, (p.s.n.), vil, 269. eas of northern Michigan, ue Ge Eby, J. H., (with C. P. Berkey), Russell, (abs.), xxxv, 177. | Oceurrence of copper minerals in Drummond, A. D., Great Lake ba- hematite ore, (rev.), xix, 417. sins of the St. Lawrence, (rev.), Eakle, A. S., Dikes near Lyon Mt., iii, 198. aN te : Clinton county, N. Y., xii, 31; Drury college, Scientific society, Erionite, a new zeolite, xxii, 378; (p.s.n.), xxxii, 400. E Topaz crystals in the U. S. Nat. Dryer, C. R., Lessons in physical | museum, (rev.), xxiii, 125; Pet- geography, (rev.), xxix, 57; Gla- | yographical notes on rocks from cial geology of the Irondoquoit the Fiji islands, (rev.), xxiv, 305; region, v, 202. pat (p.s.n.), xxvi, 195; Mineral Tables, Drygalski’s glacial studies in Green- (rev.), xxxiii, 257; land, (ed. com.), xxii, 323. : Earle, Charles, Paleosyops and al- Dual nomenclature in classification,: | lied genera, (rev.), vii, 381 H. S. Williams, (abs.), xiii, 1389; Earliest man in America, (ed. Character of the Kinderhook | ~¢om.), ix, 52; (p.s.n.), xxviii, 265. fauna, C. R. Keves, xx, 167. | Early trilobites of the Cambrian, Duck and Riding Mountains, J. B. | G. F. Matthew, ii, 1; Stages of Tyrrell, (rev.), v, 241. q Bactrites, J. M. Clarke, xiii, 37; Duffield, W. W., (p.s.n.),.xiv, 340. Protozoa, G. F. Matthew, xv, 146; Dulau and Company, (p.s.n.), xxiv, | Pleistocene deposits of Illinois, O. 825: H, Hershey, xvii, 287; Early Dumble, E. T., Geological Survey of | date for glaciation in the Sierra Texas, ist report of progress | Nevadas, W. D. Johnson, (abs.), (rev.), iii, 270; (p.s.n.), iii, 404; xviii, 61; Important results of the Texas Earth, Inierior conditions, E. W. survey, vii, 267; Second report, Claypole, i, 382; Ditto, «1, 28; Dit- Texas survey, (rev.), viii, 187; | to, J. Le Conte, iv, 38; And its (and Cummins), Double Mountain | inhabitants, Reclus, (rev.), xX; section, ix, 347; Middle Rio 119; Interior, from the standpoint Grande, (rev.), x, 65; Third an- of the nebular hypothesis, W. H. nual report, Texas survey, | Seamon, xiv, 20; Age of, (ed. Crev Jn %, 311; Grahamite | com.), xv, 382; White hot liquid, in Texas, (rev.), xi, 120, and geological time, (ed. com.), Brown coal and lignite in Texas, xxv, 310. (rev.), xi, 209; (and W. F, Cum- Earthquakes, Charleston, E. W. mins) the Kent section and Gry- Claypole, ii, 135; Causes of R. D. phaea tucumearii, xii, 309; Sauspury, iii, 182; In Nicaragua, (p.s.n.), xv, 67; Carboniferous | J. Crawtord, vii, 77; The Charles- coal in Arizona, xxx, 270. ton, C. E. Dutton, (rev.), vil, 199; Dunyte in western Massachusetts, | In Calitornia, in 1889, Keeler, G. C. Martin, (rev.), xxii, 380. (rev.), ix, 266; In Nicaragua in Duparc relief models, (p.s.n.), xxvil, 1892, J. Crawford, x, 115; Fossil 66 : earthquake, MeGee, (abs.), xi, Duration of Niagara falls, J. W. | 133: In central Jap: , < : 4 | 33; ct _Japan, B. oto, Spencer, (rev), Zui» 16/08 MS | Grev.), xii 63) OF Constantinople, Goleman ay PAW aeren Up- (p.s.n.), xiv, 340; Since the close na Vili. 306 ’ of the Glacial period, N. 8. Sha- ee Gonomena Ae iesGh OLS ler, (rev.), xiv, 396; At New York, Shaler, (abs.), xiii, 144 Sanit, Philadelphia, etc., (p.s.n.), a? ’ e/3 ’ fe 947. To ; y) . Duplication of formation names, F. pall oe agen! bel kon oe 1899, B. Weeks, xxiii, 266. | pleas mee 0; , eae 106 “199: In Duslia from the Lower Silurian of a Ww. ae ears gerd aed eet Bohemia, Jahn, (rev.), xiii, 428. Nicaragua, J. Crawilord, XXIx, viv, Dyas in N. W. Texas, J. Marcou, | 398, 399; In Socorro, R. M. Bags, Le ie ceed ae * | dry _xxxiv, 102; New Madrid, “E. 2 : me) M. Shepard, (rev.), xxxv, 180; In Eeeten Dy T- Die cere Oa ee Norway, in 4 1904, Kolderup, , ’ , = ’ 20. Dynamic metamorphism of anor- | (p.S.n.), XXXVI, 268; osytes in the Adirondacks, J. F. seis Light in the, (ed, com.), xx, ea Soa ay . 09 Lo ; Sena ean. ‘canons in and Sy- | Eastern border nape Devonian, Stirs seta Mert sta ae eas Peis ual (Am. com.), Jt, 28. : a oe (rev.), vi, -408; Eastern continental area, Devonic, a, a) ae : (Am. com.), ii, 229. Brin site Fanaa De Eastern Pe of Bae ice-sheet, C. H. ee d Pra 99K Hitchcock, xx, 27. peer mosh, Cty, ll abt Eastern outcrop of the Kansas Per- mian, Beede and Sellards, xxxvi, 83. 38 The American Geologist. Eastman, cC. R., Translation of Zittel’s History of instruction in Geology, xiv, 179; Beitrage sur Kenntniss der Gattung Oxyrhina, (rev.), xv, 267; Distribution of sharks in the Cretaceous, (abs.), xvi, 252; (p.s.n.), xvii, 60; Dor- sal shields in the Dinichthyids, (abs.), xviii, 222; Fossil fish in the Devonian of Iowa, (rev.), xxii, 237; (p.s.n.), xxiv, 134; Eaton, E. N., Winnebago meteorite, viii, 3885, : Eckel, E. C., Intrusives in the In- wood limestone of Manhattan is- land, xxiii. 122; Classification of the crystalline cements, xxix, 146. Endoceratidae of Canada, J. : Whiteaves, (rev.), xxxvi, 186. _ Echinoderma, Bather, (rev.), xxviii, 251, 299. f Eichinodermata, Mesozoic, W. P. Clarke, (rev.), xiv, 329; Of the Missouri Silurian, R. R. Rowley, Xxxiv, 269. Echinoidea, Revision by Gregory, (rev.), xi, 360. Economic geology of Ohio, E. Or- ton, (rev.), ii, 58; Survey in Geor- gia and Alabama, Spencer, (rev.), v, 185; Geological deposits, clas- sification, W. O. Crosby, xiii, 249; Geology of the United States, R. S. Tarr, (rev.), xiii, 189; Reply to Dr. Penrose, R. S. Tarr, xiii, 361; Of the Pembina region of North Dakota, C. P. Berkey, xxxv, 142; In Peru, V. F. Marsters, xxxvi, 265; Of the United States. Hein- rich Ries, (rev.), xxxvi, 321. Economic Geology, (p.s.n.), xxxvi, 380; Consolidation, with the Amer- ican Geologist, (ed. com.), xxxvi, 309. Ecuador ores, (ed. com.), xiii, 49. Educational series of rock speci- mens, J. S. Diller, (rev.), xxiii, 61. Edward Waller Claypole, (ed. com.), xxviii, 247 Effect of continental land areas on the level of the oceans adjacent, (p.s.n.), i, 388; Of cliff erosion on form of contact surfaces, N. M. Fenniman, (rev.), xxxv, 385. Egypt, Extinct vertebrates from, e W. Andrews, (rev.), xxviil, 89. Eifel tower, (p.s.n.). Iv, 254. Eighth session, Geol. Cong. Geol., Frazer, xxvii, 335. Einege Beitrige sur Kenntniss der boehmischen Kreide, J. J. Jahn, (rev.). xvii, 54. Eisen. Gustav, (p.s.n.), xvii, 123. Ejected blocks of Monte Somma, Johnston-Lavis, (rev.), xiv, 53; Elasmobranch, O. P. Hay, (rev.), XIX, | 255% Eldridge, Geological reconnoissance in N. W. Wyoming, (rev.), xvl, 392: (p.s.n.), xxxiii, 59. Elective system in the Michigan mining school, M. E. Wadsworth, December, 1905. xvi, 223; In engineering colleges, M. E. Wadsworth, xviii, 282; Electro-chemical analysis, E. F. Smith, -(rev.), vii, 3381. Elementary Geology, Chas. Bird, (rev.), xi, 60; Meteorology, Davis, (rev.), xiii, 354; Ditto, R. S. Tarr, (rev.), xix, 277; Geography, R. E. Dodge, (rev.), xxxiv, 197; Elements of geology, J. Le Conte, (rev.), vii, 260; Fourth edition, (rev.), xviii, 384; Fifth edition, (rev.), xxxii, 395; Of crystallog- lography, G. H. Williams, (rev.), ix, 208; de Paleontologie, Bernard, (reve); UX 4102 Ditton manta. (rev.), xiv, 334; of physical ge- ography, R. S. Tarr, (rev.), xvi, 392; Of strength and weakness in building stones, A. A. Julien, (abs.), xxi, 397; Mineralogy, crys- tallography, etc., Moses and Par- rous, (rev.), xxvi, 323; Ditto, 3d edition, (rev.), xxxv, 183. Elkhorn creek area of the St. Pe- ae sandstone, O. H. Hershey, xiv, Elemente der Paleontologie Stein- mann (rev.), iii, 401; Ditto. v. 183. Elevation, Isobases of post-Glacial, DeGreer, ix, 247; Average of United States. (rev.), xv. 62. Elftman, A. H. (p.s.n.),. xvi, 130, 328; Keweenawan in N. EH. Min- nesota, xxi, 90, 175; Ditto, xxil, ae St. Croix river valley, xxii,’ EI Instituto geologica de Mexico, F. N. Gould, xxxvi, 2938. Ellensburg folio, G. O. (rev.), xxxi, 255. ‘Elliptocephalus asaphoides of the qacormi¢ of Emmons. J. Marou, hs LS Ells »5R. W. Quebec group, (abs.), v, 120; Province of Quebec, (rey.), v, 243; Resources of Quebec, (rev.), viii, 394; Laurentian of the Ottawa district, (abs.), xi, 134; Importance of photography in illustrating geological struc- ture, xi, 1389; Mica in the Lauren- tian, (abs.), xiii, 214; Potsdam and Calciferous in Quebec and Ontario, (abs.), xiv, 67; (and Barlow), Canal from St. Law- rence river to Lake Huron (rev.), Smith, xvii, 250; Province of Quebec, (rev.), xviii, 387. Ellis, Mary, Index of New York Sane publications (rev.), xxxii, Elmira quadrangle, Clarke and Lu- ther (rev.), xxxiv, 324. Emerson, B. K. Porphyritic gran- iten) CabS®) 2 aan clair riaSssicmaas Massachusetts (rev.), viii, 185; Absence of interglacial conditions in New England (abs.), xi, 174; (Histo ocliteal'94 Gorse) eox Ulin uae Kansas, Udden, vii, 340. Ergussgesteine aus Smaland, O. Nordenskjold, (rev.), xvii, 179. Erian, as a term (Am. com.), Il, 227. Erionite, new zeolite, A. S. Eakle, (rev.), xxii, 378. Erosion of small basins in the pre- Pleistocene, C. S. Beachler, xii, bly) Glacial, R. S.. Tarr, xii, 147; Tertiary and Quaternary of North America, Upham, (abs.), xii, 180; Beneath deep glaciers, N. S. Shaler, (rev.), xii, 191; Dur- ing the deposition of the Bur- lington limestones, F. M. Fultz, xv, 128; of the St. Croix dalles, Warren Upham. (abs.), xvii, 260; Of the St. Croix valley, Upham, (abs.), xxii, 258: Of mountains in southern California, F. b. Wright, xxv, 326; Of the great plains and the Cordilleran moun- tain belt, xxxiv, 35. Erosive action ef ice, G. E. Culver, (rev.), xiv, 316. Errata, {, vi; Iv,-396: v, 398% vi, vi; Vile 3943) Wiis vats be, wis xis aos xiii, 444; xvi, 410; xviii, 409; xix, AZ sxx. Vit xkl,, vit xxiv; 400; XXVs 2 LOOT Pex whe! av eV 95 SEXVAL SE CVSS excsclits 402 Ecscicey wits xxxii, 494; xxxiii, 404; xxxv, 404; xxxvi, 332. Erratic Cambrian fossils in the Eocere of Marthas Vineyard, J. RB. Woodworth, ix, 2438; Boulder from the el measures of Ten- nessee, §. W. McCallie, xxxl, 44. Eruption of Manna Toa, 1899, Ed- gar Wood. xxiv, 300. Eruptives of the Archean. (Am. com.).ii. 160. 176: Of the lake Hu- ron recion. H. W. Fairbanks, vl, 162; Of Finland, (ed. com.), Ix, 40 The American Geologist. 49; Of Electric Peak, J. P. Id- dings, (rev.), xiv, 117, Epochs of the Taconie or Lower Cambrian, N. H. Winchell, xv, 295; Acid. of northeastern Maryland, C. R. Keyes, xv, 39. Eskers near Rochester, Warren Up- ham, (abs.), xi, 241; In southern New England, J. B. Woodworth (rev.), xiv, 396; In Illinois and northward, Upham, xiv, 403; In- dicating stages in the Kansan epoch in northern Illinois, O. H. Hershey, xix, 97, 237; In west- ern New York, F. M. Comstock, PSO ie alrae Esmeralda formation, H. W. Tur- ner, xxv, 168. Estimates of geologic time, Upham, (rev.), xi, 413. Etchiminian series, G. F. Mat- thew, ii, 1; Of Cape Breton, Mat- thew, (rev.), xxv, 121; Walcott’s view of Matthew xxv, 255. Etheridge, Robt, Jr., Fauna of the Hawksbury—Wianamatta = series, (rev.), Iv, 109; (and Oliff), Meso- zoie and Tertiary insects of New South Wales, (rev.), vii, 378, (p. Sadi bbe ne (eiafol ise IDS Ie Welis))é Geology and paleontology of Queensland, (rev.), xii, 266. Ethical functions of scientific study, T. C, Chamberlin, ii, 380. Ettingshausen, Baron, Tertiary flo- ra of Australia, (rev.), iv, 116. Etude mineralogique de la lher- zolite des Pyrenées, A. Lacroix, (rev.), xvi, 122; sur la metamor- phisme de contact des roches vol- Saree A. Lacroix, (rev.); xvi, 122. Euloma- Niobe (LEVEE) SOx, E2362 Eureka district, A. Hague, (rev.), xii, 264. Fauna Brogger, Europe, Geological map, (p.s.n.), xii, 66. Eurypterina, M. Laurie, (rev.), xiii, 125. Eurypterus, W. De Lima, (rev.), xiii, 284. Evans, John, (cit.), ii, 367; Pres- idential address, (abs.), xx, 201. Evans, M. C. (cit.), iv, 55, Evans, Dr. — Report on Oregon unpublished, Bo f. Shumards iv, 6. Everette, W., Purity of gold, (p.s. ey vii, 884; Origin of gold, vii, 389. Evidenges of a Glacial epoch in Nicaragua, J. Crawford, viii, 306; Of derivation of Eskers, Kames, ete., from englacial drift, War- ren Upham, (abs.), xii, 169; Of former glaciation in Labrador and Greenland, Barton, xviii,’ 379; Of Glacial action in Australia in Permo-Carbonifer- ous time, T. W. E. David (rev.), xviii, 188; Of current action in the Ordovician of New York, R. Ruedemann, xix, 367; Of glacia- tion in Labrador and Baffin land, R. S. Tarr, xix, 191; Of Epeiro- genic movements causing the Ice age, Upham, (abs.), xxii, 250; Of December, 1905. the agency of water in the dis- tribution vf the Loess, 4G. Wright, xxxiii, 203. Evolution, J. G. Martin, (rev.), Il, 431; (p.s.n.), ii, 438. Evolution of climate, James Geikie, (rev.), v, 818; In the Mammalia, W. B. Scott, (rev.), ix, 402; Hut- ton and Cuvier, precursors of Darwin;,, — (eit.)5. xX, 226s) (Of athe Brachiopoda, Agnes Crane, (rev.), xiii, 194; Of teeth in mam- malia, H. F. Osborn, (rev.), xiii» 357; Outline of development of the idea, H. F. Osborn (rev.), xv, 184; Of Australia, A. C. Gregory, (rev.) xvi, 114; Laws of climatic, Marsden Manson, xxiii, 44; Ev- olution of climates, Marsden Manson, xxiv, 98, 157, 205; An- nouncement of the theory, (ed. com.), xxviii, 816; Studies in, C. KE. Beecher, (rev.),: xxix, 182; Of climates (ed. com.), xxxili, 116; Of earth structure with a theory of geomorphic changes, JT. M. Reader (rev.), xxxiii, 190. Examination of water for sanitary purposes, Leffmann and sean, (rev.), iii, 384; Of sandstone from Augusta county, Virginia, Ave W. Miller, Jr. (rev.), xxvii) Example of wave-formed cusps at lake George, EF. N. Comstock, xxv, 192. Excursion to Sudbury, Ontario, (p. s.n.), iv, 256; across Long island, Bryson, vii, 332; Of the Geolog- ical Society (p.s.n.), xii, 206. Exhaustion of anthracite coal, (ed. com.), iii, 45. Existence de nombreux debris de Spongiaires dans le pre-Cambri- en de Bretagne. L. Cayeux, (rev.) xvi, 59. ; Exogenous. structure of Carbonif- erous trees. HE. W. Claypole, iil, - Gunes Expedition) -to) Mi St.- Bliass se: Russell, (rev.), viii, 120; To the Bahamas, A, Agassiz (abs.), xiii, 141; Scientific to Popocatapetl, J. G. Aguilera and Ordonyez, (rev.), Xvii, 330. Experimental investigation into the flow of marble, Adams and Nigeh- olson (rev.), xxvii, 316. | " Experiments on the rounding of pebbles ,T. G. Bonney (abs.), i, 260; On the constitution of the natural silicates, Clarke and Schneider, (rev.), vii, 56; De- signed to show the upward movement of glacial debris, O. Guthrie, ix, 288; Relative to the constitution of pectolite, etce., Slee and Steiger, (rev.), xxiv, 320, Explanation by Dr. Grimsby, xix, 222; Of the phenomena seen in the Becke method of determin- ing index of refraction, W. O. Hotchkiss, xxxvi, 305. Exploration of Indian Territory and Red river, R. T. Hill, vi, 253; In Alaska, vii, 33; On Grand riv- er, Labrador, Cary (rev.), ix, 402; Index, Arctic and Antarctic, (ed. com. ), are 389; In Alaska (p.s.n.), xxvii, ue Exposition, Columbian, Mines and minerals (ed. com.), xii, 376. Extension of Uniformitarianism; to deformation, W. Je McGee, (abs.), xiv, 199; Of the upper Si- lurian the Pas. de Calais, (rev.), Barrois, xxiii, 386. Extinct Perc.ary in Michigan, A. Winchell (p.s.n.y, i, 67; Volea~ noes in Colorado, A. Lakes, v, 38; Glacier of the Salmon _ River range, G. H. Stone, xi, 406. Extinction of species, Causes of. J. McCreery, v, 100. Extra morainic drift in New Jer- sey, R. D. Salisbury, (abs.,, vill, 238; Ditto, A. A. Wright, x, 207; Ditto, G. F. Wright, (abs.), x En -Todd,.-xxxill;. 86: Or- bicular of Dehesa, California, Kessler and Hamilton, xxxiv, 133. Gabbroid rocks of Minnesota, A. N. Winchell, xxvi, 151, 261, 348. he Galena nugget (p.s.n.), xii, 65; Limestone, Age of, N.H. Winchell, (abs). scdv, 208%) “Ditto tNeds bie Winchell, xv, 33; and Maquoketa series, Sardeson, xviii, 356; Ditto, ditto, xix, 21, 180, 330. Gane, H. S., (p.s.n.), xvi, 131. Gannett, Henry, Dictionary of alti- tudes, (rev.), ix, 842; Topograpn- ical work of the United States Geological survey, xi, 65, 127: Average elevation of the United States, (rev.), xv, 62; Manual of | Genera of Sauropoda founded 49 topographic methods, (rev.), xvi, 60; Dictionary of altitudes of tne United States, (rev.), xxv, 121; Origin of certain place names in the United States, (rev.), xxxi, 186; Ditto, (rev.), xxxv, 393. Gap Nickel Mine, (p.s.n.), vii, 334. Gardner collection of photographs, (p.s.n.), xvii, 340. : ; Garwood, E. J., (p.s.n.), xxvii, 263. Gas wells in Pennsylvania, E. W. Claypole, i, 31; At Findlay, O., Z, L. White, (rev.), i, 65; At Litehfield, Ul., (p:s.n.), f, 38: At San Antonio, Texas, (p.s.n.), ill, 279; Near Albert Lea, Minnesota, (D:S-n)s NIV, 126.0 At Columbia Junction, Iowa, (p.s.n.), iv, 126; Borings in Indiana, Leverett, 8; In Ohio, Leverett, iv, 11; Ohio ,Orton, (p.s.n.), iv, 63; At Freeborn, Minn., p.s.n.), v, 128; Near Letts, Iowa, F. M. Witter. ix,. 319; In Ontario, Brumell (abs.), xi, 131; In Ontario, Brum- ell, (rev.), xii, 120; Central New York, C. S. Prosser, xxv, 131. Gasteropoda and cephalopoda of the Raritan clays of New Jersey, Whitfield, (rev.), xii, 329. sre of Scientists, (p.s.n.), vl, Gates, xxxiii, 156; (p.s.n.), xxxiii 200, 395; (p.s.n.), xxxvi, 198. Gaudry, A., (rem.), ii, 367; Gpisins): viii, 240, 246. Gebirgsformen in Kiarnten, Frech, (EVE ee MI Geer, Baron de, (p.s.n.), viii, 195; Changes of level in Scandinavia, (abs.), viii, 286; (rem.), viii, 242: (rem.), viii, 246, 247: Isobases of post-Glacial elevation, ix, 247; (Git) xd, 225; Geest, W. J. McGee, xxx, 381. Geiger, H. R.. (and Keith), Blue ridge near Harper’s Ferry, (rev.), vii, 262. Geikie, A. (rem:), ii, 366; Centen- ary of Hutton’s theory of the earth, (abs.), x, 189; Text-book of geology, rev.), xiii, 66; Banded structure of gabbros in the Isle of Skye, (rev.), xv, 128; (p.s.n.), xvi, Hd ANG (psn), XxvVilip 582 eCps: n.), Xix, 223; 365; Visit to Amer- ica, xix, 424; (p.s.n:), xxxii, 332; Text-book of geology, 4th edition, (rev.), xxxiii, 51. Geikie, James, Vice presidential address, (rev.), iv, 376; Evolution of climate, (rev.), v, 313; At Bos- ton, (p.s.n.), vii, 335; Glaciai suc- in. Europe (rev.), x. 327; Glcial succession in the British Isles and Northern Europe, (abs.), xii, 224: Ice age and its relation to the antiquity of Man. (rev.), xv. 52; (p.s.n.) xvi, 180; Earth Seulnture, or the origin of land forms. (rev.), xxiii, 261; Structural and Field geology, (rev.), xxxvi, 320. Gems and precious stones, G. F. Kunz. (rev.), vi, 122; At the Co- lumbian exposition, G. H. Wil- liams, xiii, 349; (ed. com.). xiii, 415; And gem minera's, 9 C. Farrington, (rev.), xxxiii, 258. on 50 The American Geologist. December, 1905. separate bones, (p.s.n.), i, 338; Two Carboniferous, T. D. A. Cockerell, xxxvi, 330. Generic evolution of the paleozoic brachiopoda, Agnes Crane, xi, 400. Generic relations of Platyceras and Capulus, C. R. Keyes, vi, 6. General interior condition of the earth, J. Le Conte, iv, 38. Genesis of the Arietidae, Hyatt, J. Marcou, vi, 128; of iron ores by replacement of limestone, J. P. Kimball, viii, 352; of clay stones, H. W. Nichols, xix, 324; of iron ores, J. P. Kimball, xxi, 155; of bitumens, S. F. Peckham, (rev.), xxiii, 327. f Genetic relationships among igne- ous rocks, J. P. Iddings (rev.), xili, 195; and structural relations of the igneous rocks of the Ne- ponset valley, W.. O. Crosby, xxxvi. 34, 69. Gentil, Louis, Esquisse stratigraph- ique et petrographique du bassin de la Tafna (Algerie). (rev.), xxxi, 258. Genus Winchellia, L Lesquereux, xii, 209; Temnocyon and Hypo- temnodon from Oregon, Eyer- man, xvii. 267. Ceographen-Kalendar, H. Haack, (rev.), XXxXii, 255. Geogravhic features of Texas, R. F. Hill, v. 9, 68; Development of northern New Jersey, Davis and Wood, (rev.), vi, 195; Distribu- tion of fossil plants, L. F. Ward, (rev.), vi, 323; Survey west of the 100th meridian, Wheeler, (rev.), vil, 259: Illustrations for teach- ing physical geography, W. M. Davis, (rev.), xi, 416; Develop- ment of the eastern part of the Mississippi drainage basin, L. G. Westgate, xi, 245; Teaching, Im- nrovement of. W. M. Davis, (rev.), xii, 192; Development. of alluvial terraces, R. HE. Dodge. (rev.), xiv, 397; Development of the Connecticut valley, (abs.), xvi. 245; Relations of granites and porphyries, C. R. Keyes, (abs.), xvii, 91; Influences in American history, A. P. Brigham, (rev.), xxxiii, 257; Extent of Cambrian, Frech, (rev.), xxix, lal Geographic society of Chicago, (p. s.n.), xxv, 196; Ditto, (p:s.n.), xxxv, 190; Of Colorado, (p.s.n.), xXxxv, 63. Geography of the region about Devil’s lake and the Dalles of the Wisconsin, Salisbury and Atwood (rev.), xxvi, 252; New hasis. J. .Q. Redway, (rev.), xxviii, 254; Of Minnesota, C. W. Hall. (rev... OOxxii 20 sins ithe United States, W. M. Davis, xxxiii, 156; Dodge’s Advanced, (rev.), xxxv, 181; Physical Lab- oratory Manual. A. P. Brigham, (rev.), xxxv, 181. Geraraphy and resources of Sak- alin Island, B. Howard, (abs.), xxii, 261; Of Chicago and its en- virons, Salisbury and _ Alden, (rev.), xxv, 174. Geological classification and no- menclature, Jules Marcou, ii, 129; Correlation by means of fossil plants, L. F. Ward, ix, 34; Biol- ogy, History of organisms, (rev.), xvii, 187. Geological frauds, (p.s.n.), ix, 69; Myths, B. K.- Emerson, (abs.), xviii, 217. Geological. History of the Osark uplift, G. C. Broadhead, iii, 6. Of “the. Quebec group; -Ts! Flunt, \v, 212. Evolution of the mnon-moun- tainous topography of Texas, R. T. Hill, x; 105; Strueture of the Blue Ridge in Maryland and Vir~ ginia, A. Keith, x, 362. Time as indicated by the sed- imentary rocks of America. C. D. Walcott, xii, 343. Features about Atlanta, Ga., C. W. Purington, xiv, 105. Time, Length of, Fairchild, (rev Ney xv, 51; History of Missouri, 4 Winslow, xv, 81; History of Rochester, N. ve Fairchild, (rev.), xv, 50; History of har- bots; ND oS) Shaler? (neve) 26, Canals between the Atlantic and Pacific oceans, J. W. Spencer, (abs.), xvi, 248; Sketch of the Sierra Tlayacac, Mexico, A. C. Gill. .(abs.),- xvi, 240. Of the Chautauqua grape belt, RS.) Darn “Grevid) EXVin 61s Sl Sev-— enth summer meeting, Upham, xvi, 233; (p.s.n.), xvi, 329, 400; Philadelphia meeting, abstracts, W. Upham, xvii, 89; (ed. com.), xviii, 35; Buffalo meeting, ab- stracts, Upham, xviii, 213; Meet- ing at Washington, (list of pa- pers), xix, 145; Meeting at Mon- treal \(pissn-)5, xx, sb) hist eos papers at the winter meeting, New York, (p.s.n.), xxiii, 68; Re- port of the same meeeting, E, O. Hovey, xxiii, 861; Twelfth win- ter meeting, List of papers, xxiv, 395; (p:S.n.), Xxvii, 129: Ditto, Cordilleran section, abstracts, xxvii, 130; Rochester meeting, (p. s.n.), xxix, 64; Winter meeting, 1902, Washington, (p.s.n.), xxxi, 66; St. Louis meeting, (p.s.n.), xxxii, 400; St. Louis meeting, List of papers, xxxiii, 203; (p.s. Hs) pe OO Seventeenth meeting, p.s.n.), xxxv, 129. Geol. Soc. Wash. (p.s.n.), xi, 283; (p.s.n.), xiii, 76; (p.s.n.), xv, 399; (pss!) XViE’ 6% 4002 Gorse) xvii, 125, 1938, 264, 341, 344, 407: (p.s.n. abstracts), xviii, 61; (p.s. n.), xxi, 135; List of papers, (p. S100) Remi erdiqe EL SID Svidope | (Gewsiaup xxi. 397; (p.s.n.) xxiv, 391; (p.s.n.) XXV5 195,—3a0; (p-Sin:), xxvily 129, 196, 263, 327, 389; (p.s.n.), xxviii, SURIEE MGenstiogin ppo-dbc Ue Crgoustiauils xxxi, 64, 128, 198, 325, 399; (p.s.n.), xxiii, 200, 269; (p.s.n.), xxxv, 190. Geological Surveys. See under the several states. Geologist, The American, consol- idated with Eronomic Geology, (ed. com.), xxvi, 309. Geologues du Jura, J. Marcou, (rev.), iv, 186. Geology, vol. 1. Chamberlin and Salisbury, (rev.). xxxiii, 382. Geology, in the educational strug- ele for existence, (ed. com.), I. 36: And mining industry at Lead- ville, S. EF. Emmons, (rev.), i, 194. In preparatory schools, W. E. Taylor, i, 316: As a means of eulture. ti, 44, 100; Chemical, physical and stratigraphical, Prestwich, (rev.), fi. 341. Of Mt. Stevhen, British Colum- bia. R. G. McConnell, iii, 22; Of western Texas, Hill, (rev.). iil, 51: And mining of the Black Hills, Carpenter and Hoffman, 52 (rev.), ili, 202. Head of Chesapeake bay, Mc- Gee, (rev.), Iv, 113; Of south- eastern Iowa. C. H. Gordon. iv. 237: in- the High school, V. C: Alderson, iv, 284; Of New Zea- land, Hutton, (rev.) iv, 306; Of Queensland, R. L. Jack, (rev.), iv, 307; Of the Montmorenci, J. F. James, iv, 387; Interesting Nor- wegian, A. Winchell, iv, 314. Of Colorado ore deposits, (rev.) A, lakes, v, 57. Of the Lassen peak district, Diller, (rev.) vi, 196; Mt. Des- ert island, Shaler, (rev.), vi, 197. And Physiography of N. W. Colorado, (CG. A. White, (rev;); vii, 57; Of the Concho country, Otto Lerch, vii, °73; Mother Lode gold belt, H. W. Fairbanks, vii, 209: Of the Southwest, R. T. Hill, vil, 119, 254, 366; South- western New York, G. D. Harris, vii, 164. Of the Barbadoes, Jukes- Browne, (rev.), viii, 56; Environs of Quebec, Jules Marcou, (rev.), viii, 119; Ditto, H. M. Ami, viil, 186; Mont Diablo, H. W. Turner, (rev.), viii, 117; South America, Steinmann, (abs.), viii, 198; As a study (ed. com.), viii, 324; At the University of Wisconsin (p.s.n.), viii. 404. Of” ‘Columbia; ‘Bolivia,. ete: Karston, (rev.), x, 321; Of Mary- land, Williams and Clark, (rev.), x, 63; Crazy mountains, Wolff, (rev.), xX, 319. And resources of Kansas, R. Hay, (rev.), xi, 359. Geology. A. J. Jukes-Browne, (rev.), xii, 339. Big Stone gap coal fields, M. R. Campbell, (rev.), xiv, 392. Angel island, F. L. Ransome, (rev.), xv. 57; Conanicut island, G. L. Collie, (rev.). xv, 386. At-the British Association, E. W. Claypole, xvi, 300; Crucial points in the geology of lake Superior region. N. H. Winchell, xvi, 12. The alb0s. 205s 269). seis) Of “old Hampshire county. Massachu- setts, B. K. Emerson, (abs.), xvi, 238: Green mountains in Massachusetts, Pumpelly, Wolff ard Dale. (rev.), xvi. 386 of Moriah and Westport townshins, J. Ye. emp; (rev.)), xvii, 251. And mining Krahmann, (rev.), xviii, 2983: In the universities of the United States. TT: C. Hop- kins, (p.s.n.), xviii, 401. Of a typical mining camp in New Mexico, C. L. Herrick. xix, 254. St. Croix dalles area, C. P. Berkey. xx, 345. Greater New York, F. J. H. Merrill, (abs.), xxi. 72; Of the Keweenawan area in northeast- ern Minnesota, A. H. Elftman, xxi, G0Ludlth: Of Gthe 4St Croix diles, @. BP. Berkey. xxi. 139. 270: Massanuttan mountain in The American Geologist. December, 1905. Virginia, A: C. Spencer, (rev.), xxi, 197; Environs of Tammer- fors. J. J. Sederholm, xxl, 213. Environs of Albuquerque, New Mex., C) Le Herrick, xxii, 267 Of the Yukon gold district, J. E. Spurr, (rev.), xxii, 49; Ke- weenawan area in Minnesota, A. Hi. Elftman, xxii, 131; and Geography at the American As- sociation meeting at Boston, ab- stracts, Upham, xxii, 248. And physiography of the Lake region in Central America, (abs.) xxili, 94; And Archeology of Cal- ifornia, McGee and _ Holmes, (abs.), xxiii, 96; Of the Cascade mountains, I. C. Russell, (abs.), xxiii, 96; Yosemite national park, H. W. Turner, (abs.), xxiii, 100; Lake Placid region, J. F. Kemp, (rev.), xxiil, 195. Aspen mining district, J.’ E. Spurr, (rev.), xxiv, 307; Greene county, Mo., E. M. Shepard, (rev.), xxiv, 184; And Paleontol- ee von Zittel, (rev.), xxiv, Old Hampshire county, Mass., B. K. Emerson; (rev.), xxv. 51; Orizaba, E. Bose, (rev.), xxv, 315; Of New Hampshire, C. H. Hitcheock, (ed. com.), xxv, 244. At Harvard University, (p.s.n.), xxvii, 64; Of eastern Berkshire county, Mass3v Bo kk. Eimiersom, (rev.), xxvii, 59; Of the Tallulah gorge, S. P. Jones, xxvii, 67; Of the Boston basin; The Blue Hills complex, AW. Os, ‘Crosbys = (ev, xxvii, 179; Of the Little Belt mountains, Weed and _ Pirsson, (rev.); xxvii, 254; In its relations to topography, J. C. Branner, (rev.), xxvii, 257. Of the South African republic, (p.s.n.), XXVIII, | 72655 Eastern Choctaw coal fields, Taff and Ad- ams, (rev.), xxviii, 318; And wa- ter resources of Nez Percé coun- ty, Idaho, I. C. Russell, (rev.), xxviii, 310. Randhill and vicinity, Clinton county, H..P:, Cushing; -@ev-); XX 582) Of Cincinnati; Iq sev Nickles, (rev.), xxix, 181. Jemez-Albuquerque region, New Mevico, A. B. Reagan, xxxi, #7 Fort Apache region, A. B. Reagan, xxxii, 265; And water resources of the Snake _ river plains, Idaho, I. C. Russell, (rev.),- Xxxii, 121. lirder the new hypothesis of earth origin, | L. Fairchild, xxxiii, 94; Of Worcester, Mass., Perry and Emerson, (rev.), xxxiii, 122. Watkins and Elmira quadran- gles, Clarke and Luther, (rev.), xxxiv, 3824; And water resources of the Lower James valley, South Dakota. Todd and Hall, (rev.), xxxiv, 325. San Jnsé district, Mevico. (rev.) xxxv, 55: Cerillos hills, D. W. Johnson, (rev.), xxxv, 56; Shafter Index, Silver mining district, J. A. Ud- deny (rev.),.. xxxv. 183; Little . Falls, New York, H. P. Cushing; (rev.), xxxv, 250; Mount Lofty ranges, Howchin, (rev.), XxxXxv, 114; Economic of the Pembina region of North Dakota, C. P. Berkey, xxxv, 142. Applied, Congress of, (p.s.n.), xxxvi, 62; Of the Perry basin in S. E. Maine, Smith and White, (rev.), xxxvi, 127; Field course in the Appalachian region (p.s.n.), xxxvi, 198; Rosebud Indian res- ervation, A. B. Reagan, xxxviy, 230; Economic in Peru, V. F. Marsters, xxxvi, 265; Of western ore deposits, A. Lakes, (rev.), xxxvi, 319; Structural and Field, J. Geikie, (rev.), xxxvi, 320; Economic, United States, H. Ries, (rev.), xxxvi, 321. G@eeienphogeny of the coast of northern California, A. C. Law- son (rey.), xv, 387; Upper Kern basin, Lawson, (rev.), xxxv, 113. Geomorphology of the southern Zpenehians, Hayes, (abs.), xl, Geophysics, present problems, G. F. Becker, xxxv, 4. George, R. D. (p.s.n.), (p.s.n.), xxxi, 394. Orprala formation, xxvi, 259; J. Marcou, il, Georgia, University of, (p.s.n.), ii, 370; Economic Geological survey, Spencer, (rev.), v, 185; North- eastern Alabama and adjacent portions of Georgia, Hayes, (rev.) xeo223 (pisn:);. Xi, 064° Geol: sur., Paleozoic group, J. W. Spencer, (rev.), xii, 267; Coosa valley, C. W. Hayes, (abs.), xiii, 142; Fea- tures about Atlanta, Purinton, xiv, 105; Report on marbles, S. W. ‘McCallie, (rev.), .xv, 329; Bauxite mines of Georgia, Ries, (abs.), xvii, 263; Hocene stages, G DPD; Harris; (abs:), xviii, 236; Geological Survey, Phosphates and Marls, (rev.) xxi, 93: Ditto, Water powers, xxi, 196; Phenom- ena resulting from the_ surface tension of water, G. E. Ladd, xxii, 267; Cretaceous and associ- ated clays, G. E. Ladd, xxiii, 240; Report on clays, G. E. Ladd, (rev.), xxv, 249; Artesian well system, S. W. McCallie, (rev.), Tallulah gorge, S. P. Jones, xxv, 251; The geology of the xxvii, 67; Trap dikes, S. W. Mc- Callie, xxvii, 133; Granitie rocks (Conia ike Watson, xxvii, 199; Bauxite deposits, T. L. Watson, xxviii, 25: Phenocrysts in the Granite, T. L. Watson, (rev.), xxviii, 58: Roads and road build- ing, S. W. McCallie, (rev.), xxix; 56; Sandstone dikes near Col- ones S. W. McCallie, xxxil, Geotectonic and physiographic sge- ology of western Arkansas, Win- slow, (rev.), vil, 259. Geotectonische probleme, Rothpletz, (rev.), Xv, 328 Volumes I-XXXVI. 53 Gerate Troost, L. C. Glenn, xxxv, Geschichte der Geologie und Pale- pee sta von Zittel, (rev.), XXiVv, 06. Gesner, Abram, Review of his sci- entific work, G. F. Matthew, (rev.) xx, 1387. Geyserite in Nebraska, L. E. Hicks ES S. Aughey, i, 277; Ditto, ii, 436. Giant’s kettles near Christiania and in Lucerne, Upham, xxii, 291. ° GIB T atbars Paul’ Choffat,, (ren.)) Xs Gibson, A. M. Coal Measures of Blount mountain, (rev.), xiii, 284; Coosa coal field, (rev.), xvi, 260. Gigantic placoderms from Ohio. E. W. Claypole, x, 1, Gilbert, C. C., (rev.), ii, 366. Gilbert, C. H. (p.s.n.), i, 262. Gilbert, G. K (rem.), v, 381, 382, 384, 385; Lake Bonneville (rev.), vii, 132; Post-Glacial anticlines in the vicinity of Ripley and Cal- edonia, New York, (abs.), viii, 230; (rem.), viii, 242; (rem.), viii, 247; (rem.), vili, 249, 256; Bibliography by the Inter- national Congress of Geologists, ix, 64; (rem.), x, 218; Continental problems, (rev.), xii, 118; Coon butte, Arizona (cit.), xiii, 115; Chemical equivalence of crystal- line and sedimentary rock (abs.), xii, 213, (rem.), xv, 203; Gravity determinations reported by G. R. Putnam, (rev.), xv, 388; (Dp.s.n.), xvi, 131; Niagara falls and their History, (rev.), xvii, 47; (rem.), xvii, 103; (p.s.n.), xvii, 341; 5 new laccolite locality in Colorado, (abs.), xvii, 407; Algonquin river, (abs.), xviii, 231; Whirlpool,, St. David’s channel (abs.), xviii, 232; Profile of the bed of the Niagara in its gorge (abs.), xviii, 232; Underground water of the Ar- kansas valley, (rev.), xix, 57; Sketch of Jos. F. James, xxi, 1; (p.s.n.), xxii, 129; Ripple marks and cross bedding (abs.), xxiii, 102; Ice-sculpture in western New York (abs.), xxiii, 103; Re- cent earth movement in the Great Lakes region (rev.), xxiii, 126; (p.s.n.), xxv, 129, 195; (and A. P. Brigham), Introduction to physical geography, (rev.), Xxx, 123; (p.s.n.), xxxill, 60; Regula- tion of nomenclature in the work of the United States geological survey, xxxiil, 138; Glaciers and glaciation in Alaska, G. K. Gil- bert, (rev.), xxxiII, 259; (p.s.n.), xxxiv, 399; A reference library, xxxv, 126; (p.s.n.), xxxvi, 61. Gill. A. C., Sketch of the Sierra Tlayacac, Mex. (abs.), xvi, 240. Gilman, C. E. (and Branner), Stone reef at the mouth of the Rio Grande do Norte, Brazil, xxiv, 342, Gilsonite, Claypole, iv, 386. Giordano, F. (rem.), v, 209; (obit.), xi, 363. 54 Girty, G. H., Development of the corallum in Favosites forbesi, xv, 181; Mr. Sardeson and fossil tab- ulates, xviii, 332; Typical species and characters of Aviculipecten, pagel 291; Ditto,. ditto, xxxiv, Glacial, erosion in Norway, J. W. Spencer, (rev.), ji, 482; Forma- tions of Long island, Bryson, ii, 136. Origin of cliffs, W. M. Davis, iii, 14; New Theory, (ed. com.), iii, shee Erosion, J. W. Spencer, iii, Epoch, its cause, Upham, (cit.), iv, 108: Lunoid furrows, Packard, v, 104; Geology of the Irondequoit region, "©; (R.) Dryersovs 202: Period, Causes of, Upham, vi, 327; Boundary in western Penn- sylvania, G. F. Wright, (rev.), vi. 390. Sediments of Maine, G. H. Stone, vii. 136; Lakes of Canada, Upham, vii, 375; Striae older than the Quaternary in Norway, Reusch, (p.s.n.), vii, 388. Grooves at the southern mar- gin of the drift, Foshay and Hice, (rev.), viii, 186; Grooves of Kel- ley’s island, (p.s.n.), viii, 266; eet of Germany, Salisbury, ix, Geology, Progress of, (ed. com.), ix. 260. Striae in Kansas, L. C. Woos- ter, x, 131; Lakes, Shore lines, J. KH. Todd, x. 298; Succession in Europe, J. Geikie, (rev.), x, 327. Channels over divides not evi- dence of glacial lakes. J. W. Spencer, (rev.). xi, 58; Relation- ship of certain great lakes. Up- ham, (rev.), xi, 59: .Distinet epochs, Salisbury, xi, 133; Single epoch in New England, Hitch- cock, xi, 194; Man and the gla- cial period. Symposium, xi, 180; Geology of Marthas Vineyard and Long Island, Bryson, xi, 210; Succession in Ohio, iebs Leverett (rev.), xi, 413. Submergence in Scotland, Du- gald Bell. (rev.). xii. 58; Erosion, Ieee See me Seite eae oa elhok | be! America, G. F. Wright, (abs.), xii, 173, 187; Erosion in the Fin- ger lake region. D. F. Lincoln, (abs.), xii. 177; Phenomena about Madison, T. C. Chamberlin, (abs.) xii, 176; Period, Unity of, G. F. Wright (abs.), xii, 178: Night mare and the flood. H. Howorth, (ed. com:). “xti, 181.) Striae in tows. JCalvin: “sCprsine). (xi 205: Suecession in Furone and Amer- 1Gas, Misy2280) 22655 221, 200s) Deno sition of the Joess. Chamberlin, Cors.ne) = xls 2 Drift in MIll., Leverett, (abs.), xiii, 110; Ditto. Chicago. Guthrie, Cabsoe = S 4) BYAT, Halleflintas of Sweden, Nordensk- jold, (rev.), xvii, 56. Hall, ©. M., (p-S-n.), xxvi, 63: Wife and work of, Warren Upham, xxxi, 95; North Dakota Agricul- tural college survey, (rev.), xxxiii, 123; (and J. E. Todd), Geology and water resources of the Low- er James valley, (rev.), xxxiv, 325; Papers on lake Agassiz, (cit.), xxxv, 394. Hall, C. W., Southeastern Minne- sota (abs.), ix, 216; (and —&. W. Sardeson), Paleozoic formations in southeastern Minnesota (rev.), x, 182; Pre-Cambrian floor in the northwestern United States (abs); 8XVy Og) Cp S:ns) excvineera Oe Pre-Cambrian base-leveling in the northwestern states (abs.), xviii, 238; Syllabus of general ge- ology for students (rev.), xx, 823% CDsSin>) xXx, o4e5 Cand: Have Sardeson), Wind deposits of eastern’ Minnesota (abs.), xxiii, 103; Geography of Minnesota, (rev.), xxxii, 121. Hall, James, (rem.), i, 5; Paleontol- ogy of New York, vol. vi, (rev.), i, 58; Nomenclature of the Low- er Paleozoic (Am. com.), ii, 200; (p.s.n.), ii, 862; Paleontology of New York, vols. v and vii (rev.), iii, 147; Mesozoic in the south- west, (cit.), iv, 159; (and Fra- zer), Report for the Am. Com- mittee, iv, 390; Award of the Hayden medal (ed. com.), v, 234; (rem.), viii, 253; Testimon- ial of the Int. Cong. Geologists, x, 1, (plate); Oneota sandstone (abs.), x, 194:° Introduction to paleozoic brachiopoda, (rev.), x, 251; Reminiscence of Newberry, xii, 14: Coal fields of Iowa, (cit.), X