ithe i inate wi MaMeathit at reklte ie Naat Seale anv SaeMEbep. gas it hedehs! i Panerai sft Gas bit aan Usenet By tatpoed oth ah? Wes He ig Sn Hae ‘ ‘ ; rue * ee it) “- a (Ra se pie \ uy Ve M Vetin& free ce 4/55 ia) halal yi Re th fois sae tc HE abt hat t Hneaitl REM EEae dati ver ihe ite i) Hh) it ' HAN yy hi Witity seat tt pet Ht Maan ees a ‘ Wt) " ak H MAN a, daly { Hy HF 4 f ABSA Wisi) a ai eit HuHan pea a iyi? Mss Vit lit ; } Dee 8 Heit Pent ha f wae Hata 8? Ayana EE } f ‘ ‘ f ROAR { | en Hy 4 | ioe ’ He , i) iit 4 ty ; ‘ Crater HIG AUTH MI ANBEE i Wert TAR TIER Ha vuln i aa Ha t RR Laie * Ny 4 re Fhe! i ia ti Gi i hi cH HNO a 4 ry f i aM tne tatent uiNlofi He , hi it a a a at ty ve ata ww” Ww “ FM aeagewv i*+ wo. =a =e 4 a ee eet Rees le en ee | EET=_lC( \ Ayre rertes wu TAN Ro Reid dated Jor, ros wee Wwrd v © = y UE iagg ginny we : ssl AWN WW Vv. eopoeitab emma npeeee Ses eee wee, bh ae ALTE A SSEe PROF ed be Tr Ae wYN wits: Teel wees “ ANAL ayers gy aS | Sei, belbt nf . . alin ~ Sieee B ra ao) ane ate ij ‘evel we —_" | mn ag wees? | Noe ay, re! : HEL : 4 py: nratyeets ee vagus Wowie Betcosn : Sew ey ay Hap Tan ey get eT LAL UT fin | ! o Ne < 1 eye ee ts “1 : ; wy eve a Ald “Mee, Oana, LE VV 'yy des ver metnyett ee ly eusinreee ' Wren rmven fined oh eaadmy TERT I ase fait File an tO TNNDeMarccsere ONCE NTE oer oly, vere clMlUT UL ~otiitscaaten Gas ; Ue. Wate Nar ae Sree Maga Teer ary ee MM | : Mee ~~ to Ve CCD ens fe tibeh Mvredines, NTT v0 yy ae e eu, a ie . epulioenyyth in DN, 8 Ab Lad 1 LU TTIM IH rrtttany yy A vs vse, a seige 2 Serip ert TEL EE ye, prre : v a3 yet veya rep, pies MMM ascites AMUN ct hay ww Vy ew ‘ Save we rrrrry vy 400 iy th Vy ete » + ade. Joel Ong geue TP caverceveerfymeréyerutniyl DN cede, dod nin mem | UNIVERSITY OF CALIFORNIA PUBLICATIONS GEOLOGY ANDREW C. LAWSON ° AND JOHN C. MERRIAM EDITORS VOLUME X WITH 38 PLATES UNIVERSITY OF CALIFORNIA PRESS BERKELEY 1916-1918 { LIBRARY OF CONGRESS | METEIVED ' FEB 281921 DOCUMENTS vIVISION CONTENTS PAGE . The Correlation of the Pre-Cambrian Rocks of the Region of the Great Lakes, by Andrew C. Lawson.........0cccccccccccceccecseeececseceeectesevseeveeerees . A New Mustelid from the Thousand Creek Pliocene of Nevada, by Emerson M. Butterworth........ccccccccccceccceccccccecceecscevecesececvrssevevseasevevsvaseve . The Occurrence of Ore on the Limestone Side of Garnet Zones, by Joseph B: Wom pleb yey. secs. tee eccesees cts esos suede voce ssscecsesstadti ca sesv0sdsencssseoBe vests . Fauna of the Fernando of Los Angeles, by Clarence L. Moody ee . Notes on the Marine Triassic Reptile Fauna of Spitzbergen, by Carl AY VAG COs 0 he ih a eared a ea ge mer oho SAC AeMLaed eee . New Mammalian Faunas from Miocene Sediments near Tehachapi Pass in the Southern Sierra Nevada, by John P. Buwalda............ rae . An American Pliocene Bear, by John C. Merriam, Chester Stock, and @larence mie Mio o diya. ei iacs) re suscestaecoc sis cetines- seas cepues es maansseeeonae ss . Mammalian Remains from the Chanac Formation of the Tejon Hills California, by John C. Merriam ......0.00.ccccccccceccescceeeseseeeeeeserseeseenees . Mammalian Remains from a Late Tertiary Formation at Ironside, Oregon, by John C. Merriam..........0...0cccccccccecceesceeccesccestetsseessesseenseseees . Recent Studies on the Skull and Dentition of Nothrotherium from Rancho La Brea, by Chester Stock..........ccccccccccecccccsscesscnsesesecntesseeteens . Further Observations on the Skull Structure of Mylodont Sloths from Rancho La Brea, by Chester Stoek.....0...0ccccccccccceccceces ects cesecsceeeetsees . Systematic Position of Several American Tertiary Lagomorphs, by Wee RayMOMG! WICC iso cie. ss sesecss ade co yescespsscasesst gesssesnssseoeceresssssstvedecesucsecsene . New Fossil Corals from the Pacific Coast, by Jorgen O. Nomland.......... . The Etchegoin Pliocene of Middle California, by Jorgen O. Nomland.... . Age of Strata Referred to the Ellensburg Formation in the White Bluffs of the Columbia River, by John C. Merriam and John P. IB Uva cate mers: errant ars ete gee ae. aOR ar eect nes eas freer ts . Structui » of the Pes in Mylodon Harlani, by Chester Stock............0....... . An Extinct Toad from Rancho La Brea, by Charles Lewis Camp.......... . Fauna of the Santa Margarita Beds in the North Coalinga Region of California, by Jorgen O. Nomland ooo... cccceecceccec cece cceeceesetneeees . Minerals Associated with the Crystalline Limestone at Crestmore, Riverside County, California, by Arthur S. Eakle.......000c ee. : Lay nce, and Ore Deposits of the Leona Rhyolite, by Clifton W. Veit, Kammer fee cate ee cee ee epee es ec ere ecae aoe 3 . The Breccias of the Mariposa Formation in the Vicinity of Colfax, California, by Clarence L. Mood y.u.....cccccccccccceccceceseccseeseesssersetsenerseeens . Relationships of Pliocene Mammalian Faunas from the Pacific Coast and Great Basin Provinces 01 North America, by John C. Merriam.. . Anticlines near Sunshine, Park County, Wyoming, by C. L. Moody and IN Mle Ne LOM Oe terete cece ane seees amma rete rcemne ttre crane ctceewnecseesn sescanez oneness eens . The Pleistocene Fauna of Hawver Cave, by Chester Stock...........000000.. 5. Evidence of Mammalian Palaeontology Relating to the Age of Lake Lahontan, by John C. Merriam ......00..00.cccccceccecccessessecesesecessseseteserereeaes f . New Mammalia from the Idaho Formation, by John C. Merriam.......... . Note on the Systematic Position of the Wolves of the Canis Dirus Group, by John C. Merriam... ceeccceccesesscsessccesscsssevssacessesssssesseeeees . New Puma-like Cat from Rancho La Brea, by John C. Merriam............ 255 267 287 293 BY ANDREW C. LAWSON UNIVERSITY OF CALIFORNIA PRESS ie BERKELEY in hg CRUEL iG, (RETO ORAL is ag UNIVERSITY OF CALIFORNIA PUBLICATIONS Norz.—The University of California Publications are offered in exchange for eations of learned societies and institutions, universities and libraries. Complet all the publications of the University will be sent upon request. For sample copies, publications and other information, address the Manager of the University Press California, U. S. A. All matter sent in exchange should be addressed to The Department, University Library, Berkeley, California, U. S. A. OTTO HARRASSOWITZ R. FRIEDLAENDER & SOHN ; LEIPZIG BERLIN Agent for the series in American Arch- - Agent for the series in American Arc aeology and Ethnology, Classical Philology, aeology and Ethnology, Agricultural Sciences, | Economics, Education, History, Modern Botany, Geology, Mathematics, Pathology, Philology, Philosophy, Psychology. Physiology, Zoology, and Memoirs. f Geology. ANDREW C. LAWSON and JoHN C. Merriam, Editors. Price, volumes a7 $3.50, volumes 8 and following, $5.00. ae: Cited as Uniy. Calif. Publ. Bull. Dept. Geol. . Volume 1, 1893-1896, 435 pp., with 18 plates, price -....-2...-:c-cecececscecscess-se-nsesnesesesseenee $3.50 Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price ...-..ce--cceceeeceeeeeeuees $3.50 Volume 3, 1902-1904, 482 pp., with-51 plates, price: 2.422... Seee.. eee ene $3.50 Volume 4, 1905-1906,-478 pp., with 51 plates, price -2 2.222.222 eae eee $3.50 Volume 5, 1906-1910, 458 pp., with 42 plates, price shaesdhostan tere thccee tte ond r, | A list of titles in volumes 1 to 5 will be sent upon request. ; VOLUME 6. 1, The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller..._...........0----- 156 2. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern Nevada, by John C. Merriam. Part I—Geologice History..........02-..:.---:cecceceeecoseeecentee 3. The Geology of the Sargent Oil Field, by William F. Jones 4, Additions to the Avifauna of the Pleistocene Deposits at Fossil Lake, Oregon, by y Hoye Holmes) Miller’ ...).:.:5.-2-2002.-toeeoe-dueecen-teeaereds eee eee 10e 5. The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Reid 60c 6. Note on a Gigantic Bear from the Pleistocene of Rancho La Brea, by John C. a Merriam. 7. A Collection of Mammalian Remains from Tertiary Beds on the Mohave Desert, by John C. Merriam. . Nos. 6 and 7 im ONC COVOD) 22.2222 220 -csceennseonreacensseoesvocennseseccnvonacesenetoeett gett 8. The Stratigraphic and Faunal Relations of the Martinez Formation to the Chico 4) and Tejon North of Mount Diablo, by Roy E. Dickerson ............------::-csse-scesecesoe0 5e. 9. Neocolemanite, a Variety of Colemanite, and Howlite from Lang, Los Angeles County, California, by Arthur S. Halle’... 2c.) ecco cte on oneseenan create 10¢ 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. Taylor... 5e. : 11. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern Nevada, by John C. Merriam. Part Il.—Vertebrate Faunas .......0...2..---:cecceccessoeesnere te 00 12, A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, by Loye Holmes . ie Ma Mer? 22.22 -nnps tect dnnddecnennp one -cbcepcheeecer ca tctopnas tenable ctbesban snes Seat nce aaee eee We 13. Notes on the Relationships of the Marine Saurian Fauna Deseribed from the Triassic = of Spitzbergen by Wiman, by John C. Merriam. 14. Notes on the Dentition of Omphalosaurus, by John C. Merriam and Harold C. Bryant. Nos, 13 and 14 in: one,cover -......-0°7...8 ee ee 15¢ 15. Notes on the Later Cenozoie History of the Mohave Desert Region in Southeastern California, by Charles Laurence Bakker: 2-2-2122 ..cte--ssc-scneocescnes- Jeseenporsercpensessse aero —-50¢ 16, Avifauna of the Pleistocene Cave Deposits of California, by Loye Holmes Miller ... fe! "150 17. A Fossil Beaver from the Kettleman Hills, California, by Louise Kellogg yt. (oa 18. Notes on the Genus Desmostylus of Marsh, by John C. Merriam ...........22.-1..---0 repre 111 1) Rees 19. The Elastic-Rebound Theory of Earthquakes, by Harry Fielding Reid ............-22:0--- W256: jk & VOLUME 7. 1. The Minerals of Tonopah, Nevada, by Arthur S, Hakle. ......------cceccccccsnsscesescsecnseneeeeees Do 25 2. Pseudostratification in Santa Barbara County, Ce ane by George Davis Louder- | 5:5) aE er RPA EA eet PO RE Cee OE iter erdacercectctn cogacten 3. Recent Discoveries of Carnivora in the Pleistocene of Rancho La Brea, by Jo BY Fh oc «ne en SP POSE ERE PN SOM Oe es deechieberbtedco ones 4, ie. Neocene Section at Kirker Pass on the North Side of Mount Diablo, by Bruce C01 E23 nn ae ero node re nore 5. Contributions to Avian Palaeontology from the Pacific Coast of North America, by Moye Holmes: Miller. \.-2::.220:20 20.50: 8 3 De eee Pa VEAKROT UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 1, pp. 1-19 Issued April 27, 1916 THE CORRELATION OF THE PRE-CAMBRIAN ROCKS OF THE REGION OF THE GREAT LAKES BY ANDREW C. LAWSON CONTENTS PAGE ESM TPO GUE BNO Oe ee 1 Witilitveot Wentative ‘Correlations -.2 22.22.22 ceceeceeccccececee sesedeenecceeecesecesacecteaseese 2 Criteria. of Pre-Cambrian: Correlation -2....2.2..2..----. ces see-cceesccceeneceeee eocecceeeeeeeeeoee 4 Hypothesis of Two Periods of Granitie Invasion ~.......22.2..0..2..222220.22eeeece eee 5 PAS ONC AbLOMmOL | the wEypOUMCS1Stacce.2ecsesecry coca 2ec cee 0 cae cececccuce cere: qeuscc-cecestceecsate-seseseseees 6 INO EL AG ISB, CoH IEW ey tS 0 yoo 0) ee ee ee 6 South of Lake Superior 8 North of Lake Huron 10 Southeastern Ontario and Adirondacks ~.......2..2..2..2..2..22-22-22-2202-2222eeeeeeeeeee es 11 RS NU SAU AN 9 cc ee ee eee 12 Events Connected with Granitic Invasion .............2.21..2..20.2:::-20eceeeeceeeeeeeeeeeee 12 MOV ate SH Cr OM \WIMANITONGY: ce-cecescceoce--ce feces ccceeceecece cece ceecectectevecee cece ensuceeeeeeeceeceezeeceea 13 Petrographical Discrimination of the Two Granites —....2...20220..20..20222.222222002002eee- 15 Subdivisions of Time—Nomenclature <......2...0222 22.2 csceccceeceececceececcecoesorceoeseeereneaee 16 INTRODUCTION The meeting of the International Geological Congress at Toronto in 1913 seems to have marked a new epoch in the history of our ideas of the pre-Cambrian of the region of the Great Lakes. The papers which were presented at that meeting and which have appeared since then, comprising new field observations extending from Rainy Lake to the Adirondacks and embracing both sides of Lake Superior, not only indicate a renewal of interest in the problems of pre-Cambrian geology, om University of Calforma Publications in Geology [Vou.10 but they contain data and hypotheses of prime importance for the solution of those problems. A review of the results of this new work, together with the more reliable and generally accepted conclusions of earlier investigations, show a very remarkable unanimity among the students of separate districts distributed over the entire region. There still remain, of course, certain outstanding differences of opinion over questions of correlation, and particularly as to the use of terms; but if, for the moment, we disregard names and the correlations which they imply, and focus our attention on the great and fundamental fact of sequence of formations and events, an astonishing sameness of result appears in a score of districts where more or less detailed work has been done. It is the purpose of this paper to make use of this similarity of sequence, together with a new hypothesis to be formulated in the sequel, in an effort to correlate in a comprehensive way the geological history of these districts with one another. The result of this effort is sum- marized in the tabulation which accompanies the paper. UTILITY OF TENTATIVE CORRELATIONS Some writers, notably Collins' of the Geological Survey of Canada, incline to the view that we can make real progress only by abandoning for the present all effort at a general classification of the pre-Cambrian formations and concentrating our attention on particular sections which are favorable for study, and which are near enough to permit of sure correlations from one to the other; and so gradually widen an area within which a classification may be established unvitiated by the errors of distant correlation. ; This policy as voiced by Collins is a safe one for the survey to lay down, and if pursued consistently will undoubtedly lead to positive results. It is a matter for congratulation that we have this prospect of close and detailed work on the part of the Canadian geologists, and it is to be hoped that more men will engage in it. In the vastness of the pre-Cambrian terranes of Canada and the multiplicity of problems which they present, there is every justification for the survey devoting more of its energies to this field. But the method advocated by Collins, while most commendable, is not the only one which will contribute to the solution of the general 1 A classification of the pre-Cambrian formations in the region east of Lake Superior, Congrés géologique international, 1913. 1916 | Lawson: Correlation of Pre-Cambrian Rocks 3 problem. Workers in particular closely grouped fields may ignore the work going on in other fields and publish their observations as if the latter did not exist, and so, perhaps, promote the intensity of their own activity ; but this attitude after all is only an expression of the prin- ciple of subdivision of labor, and implies that others must do the equally important work of collation, comparison and generalization. Every competent attempt at generalization from a reasonable amount of data is a step in advance in so far as it corrects the errors of earler efforts. The discarded generalizations, the succession of which creates so much disgust in the minds of some, are merely hypotheses which have served their purpose and have been supplanted by others which, in most cases, are nearer the truth. The normal procedure in scien- tific progress is the modification of hypotheses, and the discarding of generalizations as expressed in correlation tables, ete., is only an ex- emplification of this procedure. The odium which attaches to errone- ous correlation tables fades away when we regard them in their true light as hypotheses put forward to stimulate inquiry as to their validity. These hypotheses are the more necessary and the more useful in geology because of the vastness of the field of observation, the expense attaching to the work, and in pre-Cambrian geology, because of an international boundary which precludes survey officers of one country from fully familiarizing themselves with the field relations in the other. These conditions make it impossible for the individual geologist thor- oughly to test a hypothesis that may explain his own particular field, and he is under the necessity of publishing it in order to secure co- operative criticism from other fields. In most other sciences the indi- vidual worker may more conveniently put his hypothesis to the test before publication, and there are in these sciences doubtless as many discarded hypotheses as in geology, though perhaps not so many have been published. Having thus persuaded myself that tentative generalizations are a useful if not a necessary part of the method of advancing our knowl- edge of pre-Cambrian geology, I shall proceed to review briefly some phases of our present knowledge of this field and to formulate still another correlation table. JI am moved the more to do this because of the recent publication of a correlation table by Allen and Barrett,’ to certain parts of which I dissent on the ground that it does not take sufficient cognizance of the relationships established in other fields. 2 Journ. Geol., vol. 23, no. 8, p. 689, 1915. 4 University of California Publications in Geology — {Vou 10 CRITERIA OF PRE-CAMBRIAN CORRELATION The table which I offer for consideration is designed to be more than an alternative to that of Allen and Barrett, in that it exemplifies the application of a principle in the correlation of the pre-Cambrian, which if true, should be of great interest and service to students in this general field. The work of Allen and Barrett on the pre-Cambrian sequence and structure of the Gogebie range is of a high order. These geologists appear to have been actuated, however, by the principle, laid down by Collins, of every man confining himself to his own bailiwick; and they do not discuss the relation of their own very important discoveries to the general problem of the classification and correlation of the pre- Jambrian. Yet, in the use of such terms as Huronian and Animikie for major subdivisions of their sequence, they imply correlations and conclusions which are at variance with the recent results of Collins? obtained on the north side of Lake Huron by methods quite as thorough and reliable as their own. Indeed, it would be difficult to find a more striking illustration of the infelicity of the exclusive method, of ignor- ing what others are doing, than is afforded by a comparison of the use of terms in the papers by Collins on the one hand and by Allen and Barrett on the other. The correlation table here presented contains fifteen columns show- ing the pre-Cambrian sequence in as many different districts dis- tributed over the region of the Great Lakes from Rainy Lake to the Adirondacks. The sequence in every district, with one exception, column XI, is practically undisputed. The columns may be placed side by side in various ways so as to suggest various correlations ac- cording to the views of the correlator and the guiding principle of correlation adopted by him. The difficulty of finding principles suffi- ciently reliable to establish correlations in the pre-Cambrian is well known. Those that have been used by geologists up to the present are chiefly: (1) The principle of lithologice similarity and the community of conditions of deposition inferred from this similarity. (2) The principle of the similarity of sequence. (3) The principle of coinci- dence of uneconformities in the sequenee. (4) The principle of irrup- tive contacts. By diligent and repeated application of these principles numerous attempts at correlation have been made, each one seeking to improve on 3The Huronian Formations of the Temiskaming Region, Canada, Geol. Sur- vey ot Canada, Mus. Bulls. nos. 8, 1914, and 22, 1916. 1916] Lawson: Correlation of Pre-Cambrian Rocks 5 its predecessor as new similarities or dissimilarities were detected, as the members of the sequence increased in number, and as new uncon- formities or irruptive contacts were discovered. The Keewatin was segregated from the Huronian on the basis of its dissimilarity and the intrusive relations of the Laurentian granite gneiss. The iron-bearing rocks of the south side of Lake Superior were correlated with the Ani- mikian on the basis of lithologie similarity and their uneconformable relation to the Keweenawan above and to an older complex below. The Keweenawan of the north shore has been satisfactorily correlated with the rocks so named on the south shore on the basis of lithologic re- semblanee. The Huronian has been divided into three parts by two unconformities discovered within the original Huronian terrane and the correlative of these parts is claimed to have been found in various districts on the basis of lithologic resemblance, sequence and ecoinel- dence of unconformities. In this way much progress has been made and our knowledge of the pre-Cambrian has advanced greatly in the last three decades. It is evident, however, when we review the literature and note the wide differences of opinion regarding the correlation of some undis- puted sequences, that the principles hitherto invoked are not wholly adequate for the purpose. When fossils were found in the limestones of Steeprock Lake in 1911, it was my hope that the same forms might be found in similar limestones on the south side of Lake Superior and so confirm the correlation tentatively adopted. This expectation, how- ever, has not yet been realized. HYPOTHESIS OF TWO PERIODS OF GRANITIC INVASION In the correlation table here formulated a new hypothesis is intro- duced and used as an aid to correlation, which, if it is true, resolves much of the doubt which has troubled students of pre-Cambrian geology. This hypothesis states that in post-Keewatin time there were two and only two periods in which great granitic batholths were developed in the earth’s crust in the region of the present Great Lakes. It is intended in this hypothesis to exclude certain acid ‘‘red rocks’’ found intrusive in the Keweenawan as not batholithic masses and as easily distinguishable ordinarily from the granites to which reference is here made. It is also intended in each batholithie period to include all of the various satellitie rocks that pertain to granites, such as pegmatites, aplites, ete., and also certain sequences in the ir- 6 University of California Publications in Geology | Vou. 10 ruptive process connected presumably with magmatic differentiation. In general, there is lttle danger of confounding the various mani- festations of batholithic development, such as a sequence of plutonic rocks from basie to acid, of one period with those of the other when both are represented in the same field. Where the batholithic assem- blage of only one period is represented in a particular field there may be doubt ; but this may usually be resolved by an appeal to other means of correlation with neighboring fields where granites of both periods are represented. Moreover, it seems not improbable that purely petro- graphical distinctions between the granites of the two periods may be recognized which will aid in their discrimination. APPLICATION OF THE HYPOTHESIS The justification of the hypothesis of two and only two granitic assemblages in the post-Keewatin rocks of the region of the Great Lakes is the fact that in the greater number of the districts repre- sented in the accompanying tabulation there actually are two granites widely spaced in time. The hypothesis states that the earlier granite in every district was formed during one and the same general period of time, and that the later granite belongs to another period, the same for all districts. These two granitic assemblages have frequently been confused by a reference of both of them to the Laurentian, but with the inerease of detailed studies their separation in time has become apparent in many districts. Northwest of Lake Superior.—In my work on the northwest side of Lake Superior in 1911 I was so impressed with the importance of this separation that, in order to secure its recognition, and so do away with the confusion which had arisen from the indiscriminate reference of all granites to the Laurentian, I proposed that the latter term be re- tained for the older assemblage and a new term, Algoman, be em- ployed to designate the later assemblage. On the northwest side of Lake Superior there are six separate and well distributed districts which have been more or less carefully studied, and for each of which we have the necessary data for the formulation of the geological] column in the proper chronological sequence. These are: Rainy Lake, Steeprock Lake, Thunder Bay, Gunflint Lake, Vermilion Lake, and the Mesabi Range. Running through all of these districts is a relatively persistent series of formations comprising conglomerate, quartzite, graywacke, 4 1916] Lawson: Correlation of Pre-Cambrian Rocks slate, and lenses of iron formation and iron ore. This is recognized in the Mesabi, Vermilion, Gunflint and Thunder Bay districts as the Knife Lake slate and Ogishke conglomerate. From Rainy Lake to Steeprock Lake, and beyond to the eastward, the series is continu- ously exposed. No one questions the identity of the series in the sev- eral districts, and it seems fairly certain that it is the product of con- tinuous sedimentation in a definite, unbroken period of time. Tem- porarily I shall refer to it as the Seine Series and to the corresponding division of time as the Seine Epoch, without prejudice to any more acceptable designation that may be claimed for it later on the basis of correlation. The present distribution of the remnants of the Seine Series, taken in connection with its remarkably uniform lithologie habit, warrants the belief that originally it must have covered an area in this portion of the region of at least 10,000 square miles as a con- tinuous body of sediments. In all of the districts named above, the Seine Series rests upon the eroded surface of a complex consisting of the Keewatin invaded by granite and granite gneiss of varying facies, with the usual accom- paniment of pegmatites, aplites and other differentiation products of batholithie development. This granite and granite gneiss may most conveniently be known as Laurentian in accordance with prevailing usage. It is therefore certain that throughout all of the studied dis- tricts in the portion of the region lying to the northwest of Lake Superior, the earth’s crust was invaded by granite in time long ante- cedent to the deposition of the Seine Series and that this granite is post-Keewatin in age. It is most probably all of the same age, Le., it was all formed in the same large division of time which, in the chrono- logical scale, may be known as the Laurentian Revolution. Now the Seine Series is, in every one of the six districts named, itself cut by granite and granite gneiss of varying facies with peg- matites, aplite and other differentiation products, constituting a granitic assemblage which, from its vast areal extent, may be regarded as a manifestation of batholithic invasion. To this granite I have given the name of Algoman in a comprehensive sense, so that the period of time in which it was formed may be known as the Algoman, a term co-ordinate with Laurentian in the chronological scale. It is thus again certain that in all the studied districts northwest of Lake Superior the earth’s crust was invaded by granite in time subsequent to the deposition of the Seine Series. It is equally certain that this Algoman granite long antedates the Animikian Series, of 8 University of California Publications in Geology — [Vou. 10 the original Animikie area, since these rocks may be observed in four of the districts resting on the eroded surface of the granite in rela- tions so clear that they have never been questioned. In the Rainy Lake and Steeprock Lake Districts the Animikian is absent. There is no room for doubt, therefore, that on the northwest side of Lake Superior the Algoman granite was formed within the space of time between the close of the Seine Epoch and the beginning of the Animikian. It is highly probable on the basis of areal continuity that in all the districts the Algoman granite is the manifestation of one and the same general disturbance and batholithie invasion of the earth’s crust. The assumption that this is so is involved in the use of the term Algoman as a designation for these rocks considered as a con- stitutent part of the earth’s crust and in the use of the same term as a designation for a subdivision of geological time. From the foregoing discussion it is apparent that the Laurentian and Algoman granites afford us two splendid datum planes along which we may correlate from district to district with a confidence pro- portionate to the validity of the hypothesis of a definite proper age for each granite. In the correlation table columns I to VI, representing the sequences in the different districts, are placed side by side with the granites arranged each on a horizontal ine. The correlation thus suggested is that which is generally accepted for the non-plutonie for- mations of the pre-Cambrian of the northwest side of Lake Superior. South of Lake Superier.—On the south side of Lake Superior four of the more important and best-known districts, namely, Gogebie, Crystal Falls, Menominee, and Marquette, have been selected for con- sideration in the correlation table. In each of these districts there is found a group of formations comprising a basal quartzite and an overlying dolomite. In the Gogebie district these are known as the Sunday quartzite and the Bad River dolomite, in the Crystal Falls and Menominee districts as the Sturgeon quartzite and the Randville dolomite, and in the Marquette district as the Mesnard quartzite and the Kona dolomite. All the geologists who have studied these districts are now agreed as to the identity of this pair of formations in all four districts and their correlation is not questioned. The quartzite and dolomite, by whatever local name known, together represent a definite stratigraphic horizon and a definite period of time. Now the quartzite in all four districts rests with a basal conglomerate upon the eroded surface of granite-gneiss which has been referred to the Laurentian, or upon the Keewatin into which the latter is intrusive. It is there- 1916] Lawson: Correlation of Pre-Cambrian Rocks 9 fore fairly certain that the group comprising the quartzite and dolo- mite is later than this Laurentian granite gneiss throughout the four districts. Resting unconformably on the quartzite-dolomite group in all four districts is another group comprising in the Gogebie district the Palms quartzite, graywacke and slate, the Ironwood iron formation, and the Tyler slates; in the Crystal Falls district the Ajibik quartzite, the Vul- ean iron formation and the Hanbury slates; in the Menominee dis- trict quartzite, Vulean iron formation and Hanbury slates; and in the Marquette district the Ajibik quartzite, the Siamo slate and the Negaunee iron formation. Here, again, there is little doubt as to the correlation of this group of variously named formations throughout all four districts. The group, with loeal voleanie admixtures, repre- sents a definite stratigraphic horizon and a definite period of time which is the same in all districts. In the Gogebie district the group is cut by the Presque Isle granite, as Allen and Barrett have recently shown,* and in the Menominee dis- trict the group is also cut by granite. It is therefore certain that, at a time later than the accumulation of this group of variously named formations, there was a plutonic invasion of the earth’s erust by granite on the south side of Lake Superior. Thus we have on the south side of the lake, as on the northwest side, two and (so far as we know) only two periods of batholithie in- vasion. The corresponding granites serve as on the northwest side to separate the geological column into three great divisions, one ante- eedent to the first granite, the second between the two granites and the third subsequent to the second granite. It is the essence of the hypothesis which I here advance as a tentative principle of pre- Cambrian correlation, that the two granite invasions of the south side of Lake Superior are chronologically equivalent to the two granite in- vasions of the northwest side, each to each. In accordance with this hypothesis the columns expressing the un- disputed sequence in the Gogebic, Crystal Falls, Menominee, and Mar- quette districts are placed in the tabulation with the two granites on the same time-horizons as the two granites of the northwest side of the lake. It follows, if the hypothesis is true, that the group of variously named formations on the south side, comprising the Tyler and Han- bury slates, the Ironwood, Negaunee, and Vulean iron formations, and the Palms, Siamo, and Ajibik formations, are the correlatives of the 4 Journ. Geol., vol. 23, no. 8, Nov.-Dec., 1915. 10 University of Californa Publications in Geology [| Vou. 10 group of variously named formations on the northwest side compris- ing the Seine slate, quartzite and conglomerate, the Knife slates, Agawa iron formation, and Ogishke conglomerate of the northwest side. It follows also from the recent work of Allen and Barrett® that the Copps Formation, the Michigamme slate, the Bijiki iron forma- tion, and the Goodrich quartzite of the south side are the correlatives of the Animikian of the northwest side of Lake Superior. North of Lake Huron.—Coming now to the Canadian territory ex- tending from Lake Huron to Lake Temiskaming, there are three gen- eral districts in each of which the sequence of the pre-Cambrian rocks has been for the most part clearly established. These are the north shore of Lake Huron, Sudbury, and Lake Temiskaming. In all three districts it is now agreed that in post-Keewatin time there were two distinct periods of granitie invasion. It is also undisputed that one of these invasions occurred in time long antecedent to the deposition of the great body of sedimentary rocks now called the Temiskamian (Sudbury) series, and that the second period of granitic invasion is later than that series. This facet was well known to Logan and pre- cisely described by him in the following words: The intrusive granite occupies a considerable area on the coast of Lake Huron, south of Lake Pakokagaming. It there breaks through and disturbs the gneiss of the Laurentian Series and forms a nucleus from which emanates a complexity of dykes, proceeding to considerable distances. As dykes of a similar character are met with intersecting the rocks of the Huronian Series (Temiskamian of Miller and Knight), the nucleus in question is supposed to be of Huronian age, ete.6 Tt seems clear that the older of these granites is what Logan called Laurentian and that it is older than the Temiskamian (Sudbury) series. The later granite cuts the Temiskamian, as is described by Logan, Miller, Coleman, and Collins. In the Sudbury district the Temiskamian (Sudbury) series is invaded by granite and the con- glomerate of the series contains boulders of granite, although the basement is not exposed. In the Cobalt district the Temiskamian rests on the eroded surface of the Laurentian granite and is itself in- vaded by the Lorrain granite. In a recent paper Collins’ has shown that the later, or Killarney, granite also cuts the Bruce series. 6 Geology of Canada, p. 58, 1863. 7 Geol. Survey of Canada, Mus. Bull. no. 22, 1916. 1916] Lawson: Correlation of Pre-Cambrian Rocks 11 It thus seems pretty certain that the territory extending from Lake Huron to Lake Temiskaming, and including the Lake Huron, Sud- bury, and Cobalt districts, suffered granite invasion at two widely spaced periods. These two periods of granitic invasion separate the sequence of epigene rocks throughout these three districts into three parts, precisely in the same way as the two granites on the south side of Lake Superior do, and it seems probable that they are chronological equivalents each to each. If this be true, then it follows that the Temiskamian and Bruce series both fall into the middle of the three great divisions of time, that is, they were deposited in the period between the degradation of the Laurentian and the invasion of the region by the Killarney or Lorrain granite. The relations of the Temiskamian to the Bruce series have not yet been satisfactorily established, but it seems probable that the Bruce series is the equivalent of the Sturgeon quartzite and Kona dolomite, ete., of the south side of Lake Superior; while it is equally probable that the Temiskamian is the equivalent of the group of variously named formations on the south side comprising the Tyler and Hanbury slate, the Ironwood, Negaumee, and Vulean iron forma- tion, the Palms and Ajibik formations, ete., and therefore the correla- tive of the Seine Series on the northwest side of Lake Superior. The Cobalt Series appears then with little question to be the equivalent of the Copps, Michigamme, ete., on the south side and of the Animikian of the northwest side. Southeastern Ontario and Adirondacks.—In Southeastern Ontario there is an older granite gneiss, the Laurentian, cutting the Keewatin and Grenville series, and a later, Moira, cutting the Hastings series, which rests upon the eroded surface of the Laurentian. These two granites, by the hypothesis here advanced, are the respective chrono- logical equivalents of the two granites on the north shore of Lake Huron, on the south side of Lake Superior and on the northwest side ; and the Hastings series is either the correlative of the Temiskamian, as Miller and Knight assert, as well as of the Tyler-Hanbury-Palms- Siamo-Ajibik, ete., and of the Seine; or the correlative of the Bruce series. In the Adirondacks, according to Cushing,* there are two granites of widely different ages, the Laurentian intrusive in the Grenville, and the Picton, itself undeformed, cutting the Laurentian after the de- formation of the latter. 8 Am. Journ. Sci., vol 39, pp. 288-294, March, 1915. 12 University of California Publications in Geology [Vou. 10 Summary.—lt thus appears that in every one of the fifteen dis- tricts, extending over a belt of the continent nearly a thousand miles long and covering both sides of the Great Lakes, we have at least one and not more than two periods of granitic invasion well established. The older granite is represented in all fifteen districts; while the later granite is found in thirteen districts, failing to appear in the Crystal Falls and Marquette, although in the last-named district more discriminating study may yet show its presence. In neither of the two districts in which only one granite is found is there any doubt as to the period to which it belongs. We may safely conclude, there- fore, that in every one of the fifteen districts, considered individually, geological time is blocked out into three grand divisions by the two granite Invasions: the pre-granitic, the inter-granitic and the post- granitic. It is the essence of the hypothesis here set forth that these three divisions of time, which are so well established in the individual districts, are the same in all of them, there being but one pre-granitie, one inter-granitie and one post-granitie period represented by the known epigene rocks throughout the entire region from Rainy Lake to the Adirondacks. EVENTS CONNECTED WITH GRANITIC INVASION Wherever the earth’s crust is known to have been, extensively in- vaded by granite, an important concomitant condition has been the uplift of the region affected and the imauguration of a prolonged period of degradation, culminating in the removal of the cover from extensive areas of the granite. Wherever in the course of time sedi- mentation resumed its sway, the resumption was not effective until the region had been reduced to a surface of low relief. The time nec- essary for the invasion of a region by granite is unknown, but it may well have been a long drawn-out process. The stripping of the cover of the granite, however, and particularly the reduction of a high region to low relief, requires a long time in the geological sense; and the interval of no deposition, between the sediments resting on the worn surface of the granite and the sediments into which the granite is intrusive, constitutes an unconformity of a major order. We may for practical purposes take the appearance of a worn surface of granite upon which as a basement sedimentary strata rest as prima facie evi- dence of a major unconformity. Now we have such a major uncon- formity well revealed on the northwest side of Lake Superior in the 1916] Lawson: Correlation of Pre-Cambrian Rocks 13 superposition of the Steeprock series upon the granite of the first, or Laurentian, invasion; on the south side of Lake Superior in the superposition of the Sturgeon quartzite upon the Laurentian; and on the north side of Lake Huron in the superposition of the Bruce series upon the Laurentian.® Similarly we have another major unconformity equally well estab- lished on the northwest side of Lake Superior in the superposition of the Animikian upon the granite of the second, or Algoman, invasion ; on the south side of Lake Superior in the superposition of the Michi- gamme (Copps, ete.) upon the second granite (Presque Isle) ; and on the north side of Lake Huron in the superposition of the Cobalt series upon the second granite (Lorrain, probably the same as the Killarney). Thus, when by hypothesis we correlate chronologically the pairs of granites each to each in the various districts of the tabulation, we are in reality correlating in every case a group of interconnected events of the first magnitude comprising: 1. The invasion of the crust by granite. 2. The uplift of the region. 3. The reduction of the region to low relief. This of course greatly strengthens the hypothesis since it increases the improbability of there having been a multiplicity of _ chronologically different granitic invasions each with its indueed uplift and prolonged period of degradation. It also justifies the use of such terms as Epilaurentian and Eparchean for subdivisions of geological time, since no sediments can have accumulated in any of the districts for a long period after each granitic invasion, these periods being re- corded in terms of erosion. Geologists who are concerned only with the sequence of rocks may dispense with these terms, but those who have to deal with the subdivision and correlation of geological time defeat their purpose if they ignore those large periods in which no sediments are known to have been deposited. DEPARTURES FROM UNANIMITY It is interesting to note that for the most part the sequences and correlations which are set forth in the tabulation are those which are generally accepted; and for the Canadian territory they represent the same general conclusions as have been published by Miller and Knight,'® except that these writers have not recognized the dual com- position of the Huronian system. There are, however, a few instances 9 Collins, Geol. Survey of Canada, Mus. Bull. 8 and 22, 1916. 10 Ont. Bur. Mines, 22, 2, p. 126, 1914. 14 University of California Publications in Geology (Vou. 10 in which the table differs from the views held by other geologists, and to these brief reference may now be made. As to sequences, it is first to be noted that Leith" is of the opinion that in the Mesabi district there is a third granite which cuts the Animikian. I have, however, in a former paper’? pointed out how doubtful the evidence of the age of this granite is and, as my skepti- cism has deepened, I have omitted it from the table. In the Lake Huron section, also, I have taken the liberty of differ- ing with Collins in his interpretation of the sequence. In doing this I feel that I have not done violence to any direct evidence which he has adduced as to the superposition of the Bruce series upon the Temiskamian. The hypothesis of two and only two periods of granitic invasion has been used to determine what the real sequence is. I have placed the Bruce series earher than the Killarney granite and the Cobalt series later, and suggest that the Bruce series lies below the Temiskamian, there being no very satisfactory evidence to the econ- trary. In southeastern Ontario there is doubt as to whether the Hastings Series is the correlative of the Bruce or the Temiskamian. In the table I have followed Miller and Knight who correlate it with the Temis- kamian. My most serious difference, however, is with Allen and Barrett, not as to the sequence on the south side of Lake Superior, but as to the correlation of the rocks there with those on the northwest side. As a result of some excellent field studies these geologists found’* that in the Gogebie district the rocks heretofore referred to the Animikian really comprise two series separated by a major unconformity, involy- ing the uncovering and degradation of the Presque Isle granite. This granite is the second of two granites which occur in the district and the major unconformity corresponds to the Eparchean Interval. Ac- cording to the principle of correlation here advanced, the rocks which follow the Eparchean Interval, namely, the Copps formation, should be correlated with the Animikian of Thunder Bay. Allen and Barrett, however, correlate the Tyler slate, ete., into which the Presque Isle granite is intrusive, with the Animikian, and make the Copps forma- tion and its equivalents post-Animikian, separated by a major uncon- formity. This correlation involves the notion of three great granitic 10.8. G. S., Mon. 43, p. 411. 12 Comptes Rendus Cong. géol. internat. XII, 1913, p. 367. 13 Journ. Geol., vol. 23, no. 8, 1915. _ on 1916 | Lawson: Correlation of Pre-Cambrian Rocks invasions in the Lake Superior districts and three major unconformi- ties, and this I hold to be a misconception of the geological history of the region. On the south side of Lake Superior the local correlations advo- eated by Allen, which I have for the most part followed in the table, are not wholly accepted by Leith. The difference of view is fully set forth in recent papers by these writers and need not be restated, since they do not affect seriously the main hypothesis of this paper. PETROGRAPHICAL DISCRIMINATION OF THE TWO GRANITES It would be a matter of great interest and importance if petro- graphical criteria could be formulated whereby the Laurentian and Algoman plutonic rocks could be discriminated ; but it is probable that our studies of these rocks are too ttle advanced to make such a dis- crimination reasonably certain. Nevertheless, since a beginning at this diserimination has to be made, I venture to offer some suggestions to this end, based chiefly on my own observations: 1. The Laurentian granite is in general more uniform and monoton- ous in mineralogical composition than the Algoman granite. 2. The Algoman granite has usually undergone magmatic differ- entiation to a marked degree and, therefore, has a larger range of facies than the Laurentian, being in many areas syenitie rather than granitic. 3. The Laurentian granite had been as a rule subject to deforma- tion before the Algoman granite came into existence, and therefore may in general be expected to show more pronounced deformational effects. 4. The Algoman granite is in many extensive areas perfectly mas- sive and unfoliated and this is rarely true of the Laurentian. 5. The Laurentian granite is in many areas bleached in appearance, whereas the Algoman granite appears fresh and in many eases reddish- colored. 6. The phenomena of viscous flow is more often exemplified in the Algoman granite than in the Laurentian. 7. The minerals nepheline, titanite, apatite, and garnet are per- haps more abundant in the Algoman rocks than in the Laurentian. 8. Intrusive phenomena at the contact with encasing rocks are usually clear-cut and pronounced in the ease of the Algoman granite and are more obscure in the case of Laurentian granite. 16 University of California Publications in Geology | Vou. 10 9. The metamorphism of the rocks eneasing the Algoman granite is for rocks of pre-Laurentian age additive to an earlier metamor- phism, and for rocks of post-Laurentian age not. SUBDIVISIONS OF TIME—NOMENCLATURE Accepting now the hypothesis of two periods of granitic invasion, there remains the question of nomenclature. This has to do with the classification of assemblages of rocks and with the subdivision of geo- logical time, and the names must be appropriate to both. I have shown that pre-Cambrian epigene rocks fall into one or the other of three grand divisions of time, and for these divisions it is clear that we must have distinctive names. For the first or pre-Laurentian division I proposed'* many years ago the term Ontarian, and this still appears to me to be the best term to adopt. It is objected by Miller and Knight*® that this term has been used as a synonym for Silurian. But this synonym appears to have been stillborn; and fortunately so, for its use would be a burdensome superfluity. The word is not mentioned in the recent work'® by Schuchert on Historical Geology ; nor is it used either in the text or in the tabulation of his more technical paper’ presented at the Toronto meeting of the International Geological Con- gress. Similarly, Ulrich appears to have no use for the term as a syno- nym for Silurian in his papers.** If these authorities on the classifi- cation of the Paleozoic and many other writers who might be cited ignore the word, we may regard it as discarded and so available for the use which I suggested in 1889. As for the substitute, Loganian, proposed by Miller and Knight,’® that is effectively disbarred by the general use of the name Logan for the sills of Lake Superior.?° Applied to the rocks formed in this period of time, Ontarian ranks as a system and embraces the Coutchiching, Keewatin, and Grenville series. For the second grand division of pre-Cambrian time the term Huronian is undoubtedly the most fitting, as well as the most thor- 14 The Internal Relations and Taxonomy of the Archean of Central Canada, Bull. Geol. Soe. Am., Dec., 1889. 15 Revision of pre-Cambrian Classification in Ontario, Journ. Geol., vol. 23, 1915. 16 Pirsson and Schuchert, A Text-book of Geology, Part II, 1915. 17 The Delimitation of the Geologie Period, etc., Cong. géol. internat., 1913. 18 E.g., Revision of the Paleozoic Systems, Bull. Geol. Soc. Am., vol. 22, pl. rap, se ALIE 19 Op. cit. 20 The Laccolithic Sills of the Northwest Coast of Lake Superior, Geol. and Nat. Hist. Surv. Minn., Bull. no. 8, 1893. ~ 1916] Lawson: Correlation of Pre-Cambrian Rocks 1 oughly established by the rules of priority and respect for the pioneer workers in this field. From the point of view of stratigraphy Huron- lan is the name of a system and embraces the Bruce Series of Lake Huron and its equivalents as well as the Temiskamian and its equiva- lents. By adopting these two terms, the first proposed by Collins*! in 1914 on behalf of the Geological Survey of Canada and the second by Miller** in 1911, we avoid the confusion which attaches to the terms Upper and Lower Huronian. Coleman** has sought to substitute Sud- burian for Temiskamian but the latter term has priority and should be retained. For the third of the grand divisions of pre-Cambrian time repre- sented by epigene rocks I propose, as I have done in previous papers, the retention of the term Algonkian. A name is needed and I know of no better use to which the term Algonkian can be put. The name is, I am well aware, in bad repute and nearly meaningless, but I hope it may be retained to serve the purpose for which it was originally intended, namely, to designate the pre-Cambrian rocks laid down in post-Archean time, and as a name for the corresponding period. Thus defined, Algonkian is a system embracing the Animikian and the Keweenawan. This system might with propriety be included in the Paleozoic, to the great simplification of our general scheme of classi- fication. The Ontarian period is separated from the Huronian by a long lapse of time in which no epigene rocks were formed in the region considered, nor anywhere else that we have cognizance of. Geological processes not less important and even more interesting than sedimenta- tion were, however, in operation; and the record of events and of the passage of time is just as clearly marked as it is in other periods by the accumulation of strata. These events, from the point of view of their distribution in time, comprise: (1) The development of batho- lithic magmas accompanied by uplift and acute deformation of the crust, and the solidification of these into vast bodies of granite. (2) The prolonged degradation of the region and its reduction to a surface of low relief. The rocks formed during the first of these two time-divisions constitute so important an element in.the structure of the earth’s crust that we can seareely discuss the problems which they present without the retention of the term Laurentian, which has been 21 The Huronian Formations of Temiskaming Region, Canada, Geol. Survey of Canada, Mus. Bull. no. 8, p. 26. 22 Kng. and Min. Journ., Sept. 30, 1911, p. 648. 23 Ont. Bur. Mines, 23, pl. 1, p. 205, 1914. 18 University of California Publications in Geology [Vou. 10 so long applied to them, and which was adopted by the International *4 some years ago. If the name be retained for the rocks, as nearly all geologists conversant with this field are agreed, it seems Committee proper and convenient to use the same term for the time-division in which they were formed. The second division of the lapse between the Ontarian and the Huronian is recorded in terms of erosion only. We have no rocks to discuss or to name. But to complete the time-scale and so keep our ideas on the subdivision of geological time clear, it 1s desirable that we should name this period, and I have in a former paper suggested that it be designated the Epilaurentian Interval.*° Similarly the Huronian is separated from the Algonkian by the time necessary for the development of the Algoman granite, with its concomitant diastrophism, and by the succeeding period in which the region was reduced to a surface of low relief. These time-divisions I have designated the Algoman’® and the Eparchean Interval.*’ The last-mentioned term is much preferable to Epalgomian suggested by Schuchert?* as a substitute for the earler name, because the interval separates the great Archean Era from the Paleozoic. There can be no doubt that historically the Huronian is a subdivision of the Archean, and its relations to the Algoman are so similar to the relations of the Ontarian to the Laurentian, that it is most appropriate to group this dual set of relations and geological conditions together under the com- prehensive term Archean. In this sense the term designates an era of time truly and characteristically archaic, even from a geological point of view. The general plan of continental growth in Paleozoic time is usually regarded as having been inaugurated with the Cam- brian, but in fact it began with the Animikian. At the close of the Eparchean Interval the vast continental platform, upon which the Paleozoic rocks rest, had been completed. The early Cambrian conti- nent of Walcott?® was but a slightly modified phase of the continent upon which the Animikian strata were deposited. It was Animikian sedimentation that ushered in the Paleozoic Era. Previous to the Eparchean Interval the physiography of the continent had been wholly different, and its growth had proceeded on other lines. Events 24 Journ. Geol., vol. 13, 1905. 25 A Standard Scale for the pre-Cambrian rocks of North America, Cong. géol. internat., XII, 1913. 26 Cong. géol. internat. XII, 1913. 27 Bull. Dept. Geol. Univ. Calif., vol. 3, no. 3, 1902. 28 Text-book of Geology, p. 445, 1915. 29U. 8. G. S. 12th Ann. Rpt., 1, 1890-91. AMBRIAN ON SOUTHEASTERN DISTRICTS vil XIV XV GocEsBic S. E. OnTaARIo ADIRONDACKS leenawan | if »s Formation | ate, graywacke, | ert, conglomerat¢ PALEOZOIC? ERA 4 EPAmr unconformity ™ ty —_—_——— lite (Presque Islei2) Granite (Moira) Granite (Picton) r slate, volcanics Hastings wood I. F., Palms nformity | | River limestone, lay quartzite Major unconformity | Major unconformity r unconformity mity =~ a ARCHEAN ERA Granite gneiss Granite gneiss lite gneiss Grenville Grenville aS Keewatin X.—Van Hise ani land Barrett, Jour! s, Geol. Survey of faght, Ont. Bur. Min aburn. Sci., vol. 39, L. DEPT, GEOL., Univ. Caurr., Vou. 10, No. 1. CORRELATION OF THE PRE-CAMBRIAN ON THE BASIS OF TWO AND ONLY TWO GRANITIC INVASIONS T ] 7 NORTHWEST OF LAKE SUPERIOR SOUTH OF LAKE SUPERIOR NORTH OF LAKE HURON SOUTHEASTERN DISTRICTS < — — — — — atk. — — — - = = : | I 1 mt Iv v vI vit vill 1x | x XI pate | XIIL xIv xv id | Rarsy LAKE STrEPROCK LaKE ‘Tuuxpee Bay Guxruint Laxe Veruiuion Lake Mrsant Goarpre CnysTaL Aus MeNosernne. | MANQUETTE Lake Huron Svppuny Copaur 8. E. Onranro Apmoxpacks 3} - —— L = ae : — —— ——— 8 KEwEENAWAny Dykes Keweenawan Keweenawan Keweenawan Keweenawan Keweenawan Dykes Dykes and Laccolith | Sills 5 | (Bpoch, Series) | A ine ss | | 4 | ANDITEIAN Animikian Animikian Animikian imiki Copps Formation Michigamme slate Voleanics, Michigamme Cobalt Series Cobalt Series Cobalt Series & | (Epoch, Series) Slates, iron formation,| Rove slate, iron Rove slate, iron irginia slate, Biwabik I. Fl} Slate, graywacke, slate, Bi LF, quartzite formation formation chert, conglomerate | Goodrich quartzite — = = = el = aoe || SE = — ————— =} — — | | | Erancuean INTERVAL Major unconformity | Major unconformity Major unconformity Major unconformity | Major unconformity Major unconformity | Unconformity Unconformity Major unconformity Major unconformity Major unconformity | ALcoMAN REVOLUTION* Granite, syenite, ete, Granite gneiss | Granite Granite Granite (Giants Range) | Granite (Giants Range) Granite (Presque Isle) Granite Granite (Killarney) Granite gneiss Granite (Lorrain) |} Granite (Moira) Granite (Picton) Se | | | — eee ae | ae athe * —— = fe = = | = 7 4 geEAT! Teenie Seine Series Seine Series | Graywacke, slate | Graywacke Knife Lake slate, Slate, graywacke, | Tyter slate, voleanies, | Paint slate, lavas, Hanbury Quinnesec schist, Hanbury} Negaunee I. F., Siamo Temiskamian Temiskamian Temiskamian Hastings i ‘© an Series) Slate, quartzite, Slate, quartzite, conglomerate, | conglomerate Agawa I. F., conglomerate Ironwood I. F., Palms slate, Vulean I. F., Ajibik Slate, Vulean I. F., | __ slate, Ajibik quartzite g ee conglomerate iron formation Ogishke conglomerate quartzite, Hemlock volcanics | quartzite Ze: |—— 4 4 = ———— = — —— — Z® | ] | z a Unconformity | - Unconformity Unconformity | Unconformity | Unconformity Unconformity | 23 |—— ——_| _——————————— — i — = —t = = — Bal Be | Steoprock Series Quartzite Wewe slate, Bruce Series 2 © | Bruce Voleanics, limestone (fossils), Bad River limestone, Randville dolomite, Randville dolomite, Kona dolomite, Quartzite, limestone, a ~ | (Epoch, Series) | quartzite, conglomerate Sunday quartzite Sturgeon quartzite Sturgeon quartzite Mesnard quartzite graywacke, limestone, 4 | | conglomerate, quartzita Ca oe] Se ee 5 | Ermavaentian Inrervat |] Major unconformity | Major unconformity Major unconformity Major unconformity | Major unconformity Major unconformity Major unconformity Major unconformity Major unconformity Major unconformity Major unconformity Major unconformity Major unconformity || Major unconformity | Major unconformity & S| Laveexrian RevonvTion Granite gneiss | Granite gneiss Granite gneiss Granite gneiss Granite gneiss Granite Granite gneiss Granite gneiss Granite gneiss Granite gneiss Granite gneiss Granite; Granite gneiss Granite gneiss Granite gneiss ] | | > | GRENVILLE | | Grenville Grenville Grenville 2 | (Epoch, Series) <2 j 5 T aa KEEWATIN Keewatin | Keewatin | Keewatin Keewatin Keewatin Keewatin Keewatin Keewatin Keewatin Keowatin Keewatin Keewatin Keewatin &| (Epoch, Series) | | Be 4 | = £ | Covromema Coutehiching | | f = Epoch, Series) | |__ (Ep I i lL | * Adams (Problems of American Geology, p. 63) takes exception to placing the Laurentian Authorities for the sequence shown in each of the columns of the tabulation: III, IV, V, VI, VII, X.—Van Hise and Leith, U. 8. G. 8. Mon. 52, 1911 } Pebbles in Temiskamian. and Algoman granites in the sequence of formations on the ground that they are intrusive fais at em = ‘VII, VIII, X.—Ath a B rt OSes G masies and not members of the stratigraphic succession. It may be urged, however, that the pepe hereon Geol. Survey of Canada, Mem. 28, 1912; Mem. 40, 1918; Cong. géol. MLDS ae st Rite com aa vol. 23, 1915. tequence is chronological as well as stratigraphic and in the standard scale we need a term n28 8h io 2h 28 OPEC TET CEM EE COLL 2G EIN BS Ch LOG EES ED for these two periods of batholithic development Perhaps the terms Laurentian Revolution III.—Smitb, Ont. Bur. Mines, 14, 1, 1905. Silver, Ont. Bur. Mines, 15, 1, 1906. Par. XIV.—Miller and Knight, Ont. Bur. Mines, 22, 2, 1914, and Algoman Revolution used in the tabulation will meet the objection. sons, Cong. géol. internat. XII, Guide Book 8, 1, 1913. XV.—Oushing, Am. Journ. Sci., vol. 9, 1915. But. Dzrr, Grou, Uwrv. attr, Vou 10, No. 1. at - Say SUT a ache Dare Meee hice eae chee aie ae Uy ae > ee i ae ant preg als WX ic 3, oer, 7 — Pe ict aids 7 ete rey ren | i ‘ i i b : 2 + Pea WE artone ¢ ETH % sien tl L ities ai i) Mereroasr ss + - ¥ eet - ee . feteaxenee ts sO EPTHT ERE IG n : y Page” daanttye CS re a3 atiges2 = ade ad “wompasoraedt SS a ro uneendas botad: tof le point gasivearA Tol becorg. eft ip seuligerigt to anvospae 2d) ah awn houre ed % | Dagistagony "stdkeemmtan he ont to t 2 ‘abios cubase oft ai bur oldqermiewe am fave. a | eT : sotvlovsh seltcewred esotd? oft gaedie® Wausuidlvsh onal saeu «aes : f - .apizoside ed} Joon Hiw aoNsloded 2 sited » 1916] Lawson: Correlation of Pre-Cambrian Rocks 19 belonged to an entirely distinct era—the Archean. Its history is a record of physical movements which cannot be discussed in terms of life, and the palaeontologists should refrain from insisting on their nomenclature in a field in which they do no work. The labor of har- monizing the views of geologists who know something of this great field is difficult enough without having to struggle with an inappro- priate classification injected by those who contribute nothing to the solution of its problems. To me the terms Archeozoic, Early Protero- zoie and Late Proterozoic*®’ are meaningless and confusing. Whatever meaning they may have to anyone is necessarily visionary ; and I ques- tion the advisability of teaching visions to beginners in geology. 30 Pirsson and Schuchert, Textbook of Geology, Pt. II, pp. 444-445, 1915. Transmitted March 30, 1916. BY. 4 EMERSON M. BUTTERWORTH > _ UNIVERSITY ve CALIFORNIA EKESS BERKELEY California, U. S. A. All matter sent in exchange should be eden Nore.—The University of Ca ‘eations of learned societies and institutions, v all the publications of the University will be se publications and other information, address the M. Department, University Library, Berkeley, California, U.S. A. OTTO HARRASSOWITZ \ tay wakes Puen aaa LEIPZIG _ BERLIN ~ Agent for the series in American Arch- Agent for the series in aeology and Ethnology, Classical Philology, - aeology and Ethnology, Agricu Economics, Education, History, Modern Botany, Geology, Mathematics, Philology, Philosophy, Psychology. Physiology, Zoology, and “Memo Geology.—AnpDREW C. Lawson and JoHN C. MzRRIAM, Editors. Price, volumes 1 volumes 8 and following, $5.00. sh * Cited as Univ. Calif. Publ. Bull. Dept. Geol. Volume 1, 1893-1896, 485 pp., with 18 plates, Price ..........csssscccsseenecessnsseeseeneeen Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price ..... Volume 3, 1902-1904, 482 pp., with 51 plates, price ...........---.s-0----- Volume 4, 1905-1906, 478 pp., with 51 plates, price .........---..-2:----+- Volume 5, 1906-1910, 458 pp., with 42 plates, price ............-....--- onc antuctenssiee A list of titles in volumes 1 to 5 will be sent upon request. i og VOLUME 6. 3. The Geology of the te Oil Field, by William F. Jones : 4, Additions to the Avifauna of the Pleistocene Deposits at Fossil Lake, Oregon, b; Leoye Holmes Miller, qu... ..::2:.:.-+.csccseteree-eoecncepsecteneetahetent sete ea ating tte neha ; 5. The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Reid 6( 6. Note on a Gigantic Bear from the Pleistocene of Rancho La Brea, by John or wf Merriam. 7. A Collection of Mammalian Remains from Tertiary Beds on the Mohave Desert, by John C. Merriam. / aig ay Nos. 6 and 7 in one cover : 1 8. The Stratigraphic and Faunal Relations of the Martinez “Formation to the Chica. and Tejon North of Mount Diablo, by Roy HE. Dickerson ...........2.2.-..ssstesseecse0 9. Neocolemanite, a Variety of Colemanite, and Howlite from Tangs) ios A County, California, by Arthur S. Wakle= S02 ee ee 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter 7 11. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northweste Nevada, by John C. Merriam. Part Il.—Vertebrate Faunas ........--2-:seces--cosee 12. A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, by Oye Holme SI 1) Sipe eee ae ER ce eats ioe ee ah he io cece 13. Notes on the Relationships of the Marine Saurian Fauna Described from the ce of Spitzbergen by Wiman, by John C. Merriam. 14. Notes on the Dentition of Omphalosaurus, by J ohn C. Merriam and Harold ©. o. Bryant 4 Nos. 13 and 14 in ONE COVET ~.-- nnn enn an -nnenn ante nnnneneence ence cneneceeeec ene rcreneecnenneneecenennee 17. A Fossil Beaver from the Kettleman rails, Golfers, by Louise Kellogg 18. Notes on the Genus Desmostylus of Marsh, by John C. Merriam ............. 19. The Elastic-Rebound Theory of Earthquakes, by Harry Fielding Reid . vou 7. . Recent Discoveries of Carnivora in the Pleistocene of Rancho La Brea, by IMG TYAN ™ Vec:.1,.0---e-nnsnspdnecnon ese seusegnedepe ste ica ena ate meets ae eS eee en - The Neocene Section at Kirker Pass on te North ‘Side of Mount eens Ta, Clark nee eeseeeenessssecssenecneneneeeneeceenentecsacnten Cees oe meen RE NY 3 7 PF pe UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY = — Knsoniaa (agg Vol. 10, No. 2, pp. 21-24, 1 text-figure Issued October 3, 1946.(\80! ai SHEEN 2 (7) a) sy 4 ta ? % OCT 131916 & Cae nal Muse’ 4 See y A NEW MUSTELID FROM THE THOUSAND CREEK PLIOCENE OF NEVADA BY EMERSON M. BUTTERWORTH The collections made by the University of California expedition to the Thousand Creek region of Nevada in the summer of 1915 inelude a mustelid form differing markedly from previously known types. It is desirable to place on record a description of this addition to the Great Basin fauna in order that the information may be available for studies involving the whole faunal assemblage of the Thousand Creek Pliocene. The writer wishes to express his appreciation for the kind criticism and guidance of Professor John C. Merriam, under whose direction this work has been executed. TAXIDEA NEVADENSIS, n.sp. Type specimen an imperfectly preserved mandible, with P,, M,, and M.,; no. 22290, Univ. Calif. Col. Vert. Palae.; from the Thousand Creek Pliocene of Thousand Creek, Nevada. Diagnostic characters: teeth robust, P, with accessory cusp posterior and external to the protoconid; protoconid, paraconid, and metaconid of M, forming an approximately equilateral triangle, with the cutting shear poorly developed; heel of M, large, with peg-like hypoconid, and well-developed entoconid; M, nearly circular in cross-section, but with four imperfectly developed tubercles. The new mustelid form is known by a single mandible, specimen 22290, representing an animal intermediate in size between the Recent badgers and the martens. Due to the fragmentary nature of the material, discussion of generic and specifie characters must be con- fined to the dentition. Imperfect preservation also precludes the 22 University of California Publications in Geology [ Vou. 10 submission of any but inferential data regarding the teeth anterior to Py. Judging from the crowding of the entire dentition anteroposteri- orly and the difference in size between the root of P, and the alveolus of P,, it is to be assumed that the premolars of specimen 22290 have suffered reduction in number and dimensions, consisting in part in the elimination of P,. P,, the sole complete representative of the premolar series, is robust and possesses a cusp posterior and external to the protoconid. This cusp is prominent in the Proeyonidae and other carnivore phyla, but seems to reach its highest development in the mustelid genera Martes and Taxidea. ALAN TL MA Wy THR Fig. 1. TLaxidea nevadensis, n. sp. Type specimen, no. 22290, X 2. Outer and occlusal views of lower dentition. Thousand Creek beds, Thousand Creek, Nevada. M, is heavy and possesses a rudimentary shear. The paraconid and protoconid are of equal size, and with the slightly smaller meta- conid form an approximately equilateral triangle. The paraconid is clearly mediad of the median anteroposterior line of the tooth. The heel of M, is larger than that observed in any of the described mustelid forms with the exception of Meles, the Old World badger. The heel is somewhat trilobate in form. The hypoconid and entoconid are exceptionally well developed, and the posterior region is elevated to form a horseshoe-shaped ridge. M, is nearly circular in cross-section, and probably single-rooted. It is inserted at an angle of about 15° to the occlusal surface of the heel of the carnassial, bringing its crushing face mediad of the median anteroposterior line of the dentition. This character is possibly at- tributable to individual variation. The crushing surface of the tooth 1916] Butterworth: A New Mustelid 23 is basin-like and irregularly cuspate around the periphery, with the protoconid, metaconid, hypoconid, and entoconid faintly defined. The unmistakable differences presented by the second lower molar are sufficient to separate the new mustelid from the Proeyonidae, the only other phylum of the Carnivora possessing characters close enough to justify comparison. Though there can be no question as to its mustelid affinities, the Thousand Creek form seems markedly different from any other representative of the group. Resembling the modern badgers in its generic characters, specimen 22290 shows the following noteworthy contrasts to the Recent Taridea tarus neglecta of North America: (1) The heel of M, of the Thousand Creek form is rela- tively larger in every dimension than the heel of this tooth in Taxidea. (2) In Taxidea the tubercles of the heel are much more highly speei- alized for a cutting function. (3) In Taridea the metaconid is slightly less prominent and is posterior to the protoconid, while the metaconid of the fossil tooth is located nearly as far forward as the protoconid. The general structure of the carnassial is, however, much alike in the two forms, and the structure of the last premolar is identical. Fundamental differences exist between the fossil mustelid and Meles. The simple spike-like P, of the Old World badger is in marked contrast to the bicuspate P, of the form from the Thousand Creek. The former has the cutting shear of the carnassial well developed, the latter exhibits a more primitive structure of this part of the tooth. In Meles the metaconid of M, is situated far posterior to the proto- conid and the markedly basin-like heel is cuspate only around the border of the tooth, while the metaconid of the fossil tooth is located almost as far forward as the protoconid, and the heel has no pro- nounced basin. Lutra, Lutreola, and Mephitis possess dental characters widely divergent from those of the Thousand Creek mustelid. These char- acters preclude any possibility of close relationship to the form under discussion. The fossil form resembles Taxidea in the structure of the lower carnassial and of P,, though there occur notable differences of pro- portions. It resembles Meles in the ratio between the heel dimensions and the anterior portion or triangle of the carnassial, but differs from the latter form in the conformation of the heel of this tooth and also in respect to the number of cusps of P,. It is evident that the Thousand Creek form is more closely related to Taxidea than to Meles, as differences of structure are of higher rank 24 University of California Publications in Geology [ Vou. 10 than differences of proportion. This conclusion is consistent with the evidence of geographical distribution. Meles is an Old World type; Taxidea, a genus characteristic of the New World, is found living in the region where the fossil form occurs. While the structure of the specimen from the Thousand Creek shows close relationship to Taxidea, the difference existing in the conformation and proportions of the heel of M, indicate that the fossil form represents a group distinct from the modern American badgers. While it is probable that a new eroup of at least subgeneric value has been here described, definite classification must await more complete structural representation. MEASUREMENTS T. neva- densis Type specimen, T. taxus (a) M. taxus (6) Thousand Recent, Recent, Creek California Germany Length anterior side P, to posterior side M, ............ 18.5mm. 29 29 Pe PaAMLeLOPOSLETION Cale Cis see cess eseee ee eens eermnees 6 9 Upk M,, anteroposterior diameter .............-..--------s--00e--eeeee 9.5 14 16 M,, transverse diameter at protoconid ... 5 6 5.5 M,, anteroposterior diameter of heel 5 5 7 M,, transverse diameter of heel ..........20222222.22..2ee eee 4.5 6.2 7 (a) 4937 Mus. Vert. Zool. (b) 21980 Mus. Vert. Zool. Transmitted March 10, 1916. er abe BULLETIN OF THE DEPARTMENT oF eee te GEOLOGY! ta “ 0, No. 3, pp. 25-37, 10 text-figures Issued © Cteben dit.) 49 Pps a ee ae = 7 % _ re a a Nene % OCT 2419655 oe “onal Mus® E OCCURRENCE OF ORE ON THE LIME- _ STONE SIDE OF GARNET ZONES tee Be es m4; BY | ve ae JOSEPH B. UMPLEBY UNIVERSITY OF CALIFORNIA PRESS BERKELEY ; UNIVERSITY OF Nore.—The University of California Publications atts tations of learned societies and institutions, universiti raries. Wy all the publications of the University will be sent upon eq For : m publications and other information, address the Manager of the ‘Univer Tsi California, U. S. A. All matter sent in exchange should be addressed Department, University Library, Berkeley, California, U. S. A. he fi OTTO HARRASSOWITZ . R. FRIEDLAENDER & Ss LEIPZIG BERLIN: Agent for the series in American Arch- aeology and Ethnology, Classical Philology, a Eeonomics, Education, History, Modern Botany, Geology, Scan ; Philology, Philosophy, Psychology. Physiology, Zoology, and Memoirs. Geology.—Anprew C. Lawson and JoHN C. Mergiam, Editors. Price, volumes 1: volumes 8 and following, $5.00. cats ae Cited as Univ. Calif. Publ. Bull. Dept. Geol. Volume 1, 1893-1896, 435 pp., with 18 plates, price -......-.--.-cssosessrateneeas ee Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price -.......-.-c-:.-0--0-- Volume 3, 1902-1904, 482 pp., with 51 plates, price -......22----c:c--ceocesssserenenses Volume 4, 1905-1906, 478 pp., with 51 plates, price ...... Volume 5, 1906-1910, 458 pp., with 42 plates, price -......-..22.----ceccecteceetoceeeees A list of titles in volumes 1 to 5 will be sent upon request. VOLUME 6. . The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller. oe . Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Nortinvestess Nevada, by John C. Merriam, Part I—Geologie History...0 ccc crseerceeees The Geology of the Sargent Oil Field, by William F. Jomes .0....-... 2 cesceseesorceneseesoes Additions: to the Avifauna of the Pleistocene Deposits at Fossil Lake, Oregon, iy Loye Holmes Miller ; PO por | 5. The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Reid F( at 6. Note on a Gigantic Bear from the Pleistocene of Rancho La Bee by at Cc. ' Merriam. at 7. A Collection of Mammalian Remains from Tertiary Beds on the Manse Desert : by John C. Merriam. \ ; Nos, 6:and 7 in one Cover 2.2 c..etetcseetsececepenneaceensneuceortneresns ae fs el 8. The Bieatioraphic: and H'aunal Relations of the Martinez Formation to the Chico — aud Tejon North of Mount Diablo, by Roy E, Dickerson ..........2-:.--.s::sc---neeeenesns vy 9. Neocolemanite, a Variety of Colemanite, and Howlite from Lang, Los Angeles County, California, by Arthur S. Boake topo tcl rr 4 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. Taylor. Bs 11. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern Nevada, by John C. Merriam. Part Il.—Vertebrate Faunas ............2.:cscssec-0s 12. A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, by Loye Holmes MTN OF i225 nas. nse snctttecd_-ncesutenpesgusessensteentronecvonen bared banat eceneientrh ont an arte 13. Notes on the Relationships of the Marine Saurian Fauna Described from the risa of Spitzbergen by Wiman, by John C. Merriam. 14. Notes on the Dentition of Omphalosaurus, by John C, Merriam and Harold G: Bryant. Nos, 13 and 14; in, one Cover, 222.220 o2 spin -no- cose os Sarpe nwa an pease ‘ 15. Notes on the Later Cenozoic History of the Mohave Desert Region in Southeastern California, by Charles Waurence Bakker 2.22 ici teseesesecnnones=sesranenpeneeer en eco neecaareas Eos 16. Avifauna of ‘the Pleistocene Cave Deposits of California, by Loye Holmes Miller 17. A Fossil Beaver from the Kettleman Hills, California, by Louise Kellogg .. 18. Notes on the Genus Desmostylus of Marsh, by John C. Merriam ................0-2- . The Elastic-Rebound Theory of Earthquakes, by Harry Fielding Reid ........ -_ = Ne} \ VOLUME 7. The Minerals of Tonopah, Nevada, by Arthur S. Hakle i . Pseudostratification in Santa Barbara County, California, by George Davis Lou é . Recent Discoveries of Carnivora in the Pleistocene of Rancho La Brea, by To on ¢ BY U5 oe: 11 Vea mee EL AI oo RN Aa SS es etree neceos ‘ . The Neocene Section at Kirker pa on: the North Side of Mount Diablo, by Bru Bay Clare cosccd ic soccceseascecesdensnnnscuqenapseancaehoetecedt baeae etme ete ase Seana ry . Contributions to Avian Palaeontology from the ‘Pacific Coast of North Ame! ica, | Loye Holmes Miller ; e nan PF wo NE ane | Fis) Bia UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY sae Vol. 10, No. 3, pp. 25-37, 10 text-figures Issu QerseOud! 44, QTE Ve THE OCCURRENCE OF ORE ON THE 7GEAE- STONE SIDE OF GARNET ZONES* BY JOSEPH B. UMPLEBY CONTENTS PAGE PUATVET © GUILT 110) Vitesse neers cee ae fee Smee oes Serene eset pe nee co ave coeccateceeee esate 25 RS SPEN SNE eWay a Co Ooh Rs ee ee ee See 26 HEPATIC S Mee oe ce ccns sores aensesy ce seSe estes te icne deca. Settee dig .2 ot eecccee_asactacec aivisssascaseedeuaZs dep$eceaseeeee=s 26 VWyeiisiotrrayfestegoyral NOFA of fe G0) NE hese epee peer ees ee ee eee 26 SS TViO Ts CLIMBAWIZ 0 10 ee eteaee ae oe aces eee Ae ce Bees pees aes erate eee eerie a zeeven eet ee ee ee ee 27 RL SAY Ee eT BXe a FS (GGT aa) em 28 AVie lar dle iia VIC XA CO oe scence aren ceca nen ee eng ee ve, Fe ee Se ae ey eae se eee cee 29 1D YOM Kay tetsh TY EB T= BN Ero CY 0 Wee ea rep OP eo 31 TAN WC Es UM a ee ee a Ee SE ee 33 Wwalmibehorsex@ opp eres elitis Yuko yess saree aera weer tees ces ced aoe eee Pocezeeee 33 MbMIG ETO TE LAGL OM gorse ee eee eres acne saee cess ss 22s esac Seon stat oeczcttgse $= sects soavscsoecasddecccacstetvees2s 35 Summary amd ‘Conclusions <2... ccececc ec ceccee cesses ceeceee cen saees sete seeveeeeseeseeeees eeeeeee ines 37 INTRODUCTION Contact metamorphie ore deposits comprise a type of particular interest because in their geologic occurrence and mineralogical makeup they are intermediate between normal fissure veins and magmatic segregations. During the last sixteen years much attention has been given to them by students of ore genesis and ideas concerning their origin have passed through many stages of development. Their general occurrence at or near igneous contacts affords the common ground that they are genetically related to intrusive masses, but concerning the details of this relationship wide diversity of opinion exists. Does the intrusion merely supply heat to the meteoric circulation, or does it supply the metamorphosing solutions? Is the metamorphism * Published by permission of the Director of the United States Geological Survey. oN 26 University of California Publications in Geology [ Vo. 10 coincident with intrusion, or subsequent to the solidification of a’ magma shell? Does the magma supply silica, alumina and iron for the lime silicates, or are these concentrated from the invaded rocks either by a reduction in volume or by meteoric waters approaching the contact? Is the attack of meteoric waters on the solidified but still hot intrusive an important factor? Does the metasomatism proceed by constant volumes? Do the lime-silicates and sulphides develop simultaneously and have they a common source? These are the prin- cipal questions now under discussion. Each of them seems to have been answered satisfactorily for individual deposits, but the problem remains how far one pattern may fit the many known occurrences, and what factors determine diversities within the type. Any adequate conception of the genesis of contact deposits must be based on the constant relationships which they exhibit, but must be sufficiently elastic to allow for observed diversities. Thus, to add either descriptions of peculiar features of individual deposits, or to point out relationships so often recurring as to be scarcely fortuitous, is to make a contribution to our knowledge of the subject, even if the genetic significance be not fully comprehended or be incorrectly stated. STATEMENT OF THESIS This paper is an endeavor to point out a common, perhaps a general, spacial relationship between ore and garnet zones in the con- tact deposits of the North American Cordillera. It is certain that in many deposits the ore bodies favor the limestone rather than the intrusive side of the garnet zone. In several places the ore comes directly up to the igneous contact, but so far as is known to the writer no clear occurrence has been deseribed where barren lime-silicate rock continues outward far beyond such ore. In the case of engulfed blocks of limestone which have suffered metamorphism the limestone side of the garnet mass is toward the central part of the block, and here ore is found in several localities. In some of these cases all of the limestone has disappeared but the ore is centrally situated. In the following paragraphs this relationship is pointed out in brief descriptions of several contact deposits, and finally its bearing upon modern theories is suggested. EXAMPLES Washington Camp, Arizona—The ore deposits at Washington Camp occur locally on the border of a great island-like mass of lime- 1916] Umpleby: Ore on the Limestone Side of Garnet Zones 27 stone surrounded by granitic rocks comprising the main part of Patagonia range.‘ The sedimentary beds dip and strike diversely in different places, but the dip is prevailingly westward at angles of 30 to 90 degrees. The deposits are tabular replacements in limestone both remote from and near to the igneous contact ‘‘and have not been observed in any instance to extend ever so slightly into the surround- ing granite.’’ The common gangue is garnet, with which the metallic minerals, chalcopyrite, sphalerite and to a minor extent galena, are intimately associated. It is particularly noteworthy, however, that ‘“‘the ore-body accompanying a contact garnet zone is always on the inside of the zone, that is, between the main body of the garnet ledge and the limestone, and not between the garnet ledge and the granite.’’ ? Crosby* states further that ‘‘obviously enough, the ores, as we now have them, are due to a metasomatic impregnation and replace- ment of the limestone against and in the massive garnet ledge.’’ The deposits of Washington Camp, therefore, clearly exemplify the formation of ore on the limestone side of garnet zones. It is per- haps worthy of note that here there has been no endomorphism, a feature in which these deposits are different from several of the others which are described. Silverbell, Arizona.—In the Silverbell district is a series of lime- stone blocks of Paleozoic age completely surrounded by alaskite, alaskite porphyry, biotite granite, andesite and quartz porphyry, in- truded in the order named.t The intrusion of the alaskite porphyry and the biotite granite was followed by intense sericitization and silicification of these rocks and by the development of great masses of garnet, quartz and wollastonite in the adjacent limestone. ‘‘Follow- ing close upon these solutions came metal-bearing magmatic waters, which impregnated porphyry, granite and alaskite with cupriferous pyrite, and deposited in the garnet zones chalcopyrite and copper- bearing pyrite that make important bodies of contact metamorphic ores.’’ Veins containing lead-silver ores also occur. Endomorphism is represented by a widespread silicification of the intrusions and a local development of garnet and epidote of igneous-rock derivation. The common section from the boundary of the intrusive rock to the limestone is ‘‘three to ten feet thick, of solid garnet and quartz, with 1Crosby, W. O., The Limestone-granite contact-deposits of Washington Camp, Arizona, Trans. Am. Inst. Min. Engrs., vol. 36, pp. 626-646, 1906. 2 Crosby, W. O., op. cit., p. 632. 3 Op. cit., p. 641. _4#Stewart, C. A., The geology and ore-deposits of the Silverbell Mining District, Arizona, Trans. Am. Inst. Min. Eners., vol. 43, pp. 240-290, 1912. 28 University of California Publications in Geology [ Vou. 10 varying amounts of wollastonite, and microscopic diopside. This is gradually replaced by garnet rock with veins and bunches of marble, and the latter becomes more abundant until we find marble with lenses and stringers of garnet and associated minerals, and these become less numerous until a pure marble remains.’’*® ‘Parts of an ore-body may be one hundred feet or more from an intrusive rock; but some portion of every ore mass is close to the contact with one of the two above-named igneous rocks. Usually there is a five to ten-foot band of garnet rock between ore and porphyry.’’* ‘‘The ore-minerals ‘are definitely later than most of the gangue-minerals, and occur com- monly as veinlets in the garnet-quartz-calcite mass, or disseminated through it.’’ 7 Seven Devils, Idaho—The rocks of the Seven Devils district comprise slate, quartzite, limestone and a vast amount of associated greenstone invaded and metamorphosed by a quartz diorite phase of the Idaho granite and capped locally by Columbia basalt.8 The ore deposits are in typical contact zones situated in part along the external contact of the quartz diorite but principally adjacent to engulfed blocks of limestone. Garnet, epidote and quartz are abundant gangue minerals and bornite and chalcopyrite are the principal sulphides. In the Queen, Blue Jacket and Arkansas mines the ore occurs on the lime- stone side of garnet zones across which veinlets of chalcopyrite and bornite in a quartz gangue connect with the igneous mass on a dip of about 15 degrees. Mining development along these veinlets has ceased in most places at the igneous contact, but they are known to extend locally twenty-five or thirty feet into the quartz diorite without notice- able diminution in size or change in character. One locality where the veinlets are particularly well shown and are closely spaced is in the Queen No. 1, Intermediate stope. See figure 1. In the Peacock Mine the ore occurs in the central part of a large garnet-epidote area bordered on the east and west by diorite and on the south by a green porphyritic rock believed to be an engulfed portion of the greenstone series. The main sedimentary contact les a few hundred feet to the north across an area of normal diorite. Thus it is suggested that an engulfed block of limestone ‘determined 5 Stewart, C. A., op. cit., p. 272. 6 Ibid., pp. 280-281. 7 Ibid., p. 282. 8 Lindgren, W., The gold and silver veins of Silver City, De Lamar and other mining districts in Idaho, Twentieth Ann. Rept., U. 8. Geol. Survey, Pt. 3, pp. 249-253, 1900. Umpleby, J. B., Reconnaissance examination, 1915. Re- port in preparation. 1916] Umpleby: Ore on the Limestone Side of Garnet Zones 29 the development of the garnet-epidote mass at the Peacock Mine, a suggestion confirmed by the occurrence of marble in diamond-drill cores which come from the deposit, although the location and direction of the hole is not known to the writer. The point of particular interest is that the ore-body occurs in the central part of the garnet mass. The Seven Devils deposits exhibit both exomorphism and endo- morphism, the latter being clearly shown by the stringers and replace- ment bodies of epidote in the diorite several feet from limestone contacts. Velardena, Mexico—The Velardena district is an area of folded Cretaceous (?) limestone overlain by andesitie tuffs and flows and traversed by andesitie dikes.° The principal intrusive rocks are dikes vv y QUARTZ DIOR! v Vvuvey SCALE OF FEET s Fig. 1. Transverse section showing relations of ore to limestone and quartz- diorite in Intermediate Stope, Queen No. 1 Mine, Seven Devils, Idaho. and necks of alaskite and trachytie alaskite accompanied or closely followed by extensive injections of dioritie rocks. All of the intrusive rocks have caused metamorphism and at a time ‘‘definitely subsequent to intrusion,’’ as shown by extensive endomorphism. The ore deposits are of varied character and clearly indicate successive stages of depo- sition. ‘‘Sulphides began to be deposited with the lime-silicates, but the chief sulphide deposition followed the lime-silicate period directly, with quartz as principal gangue.’’!” The Copper Queen is the principal copper ore-body of the district and consists of three main pipes in metamorphic rock at the contact of the diorite intrusion. The principal sulphides are cupriferous 9 Spurr, J. E., and Garrey, G. H., Ore-deposits of the Velardena District, Mexico, Econ. Geol., vol. 3, pp. 688-725, 1908. 10 Op. cit., p. 724. 30 University of California Publications in Geology [ VoL. 10 pyrite, sphalerite, and galena. The relation of the ore to garnet rock and limestone in this deposit is clearly shown by Prescott in the illustrations reproduced as figures 2 to 5.11 Prescott uses these figures to illustrate the occurrence of ore at points where limestone projects vv i vey, YVV4 "v a7 OLA es vite yy set Paley vv UPPER HORIZON INTERMEDIATE HORIZON Fig. 2. Fig. 3. LOWER HORIZON DEEP HORIZON Fig. 4. Fig. 5. CGR ATT? LIME ORE pee) ENS MONZONITE| “y vv” METAMORPHIC ROCK ve YN Generalized plan of ore chimney at Copper Queen Mine, Velardefia, Durango, Mexico. After Basil Prescott, Econ. Geol., vol. 10, p. 62, 1915. 11 Prescott, Basil, Some observations on contact metamorphic deposits, Econ. Geol., vol. 10, pp. 55-69, 1915. 1916] Umpleby: Ore on the Limestone Side of Garnet Zones All into the intrusive mass, but they are also most pertinent to the present discussion. In figures 3 and 4 the occurrence of ore on the limestone side of the lime-silicate zone is evident. In figure 5 the central lime- stone has been changed to ore, but its former extent into the area now ore is clearly shown by the relations at the top and bottom of the figure. In figure 2 the ore occurs in the central part of a lime-silicate mass which in the plane of the section is surrounded by the intrusive rock. Dolores Mine, Mexico.—The Dolores Mine, near Matehuala, 8. L. P., Mexico, is situated in an area of Mesozoic limestone, overlain by shale, which forms a great half-dome down faulted on the east..? Cutting the sedimentary rocks in the central part of the field are two masses of quartz monzonite. Both of the intrusives have caused noteworthy metamorphism, but about the northern, or Cabriza body, contact rock is especially abundant and widespread. The contacts of the intrusive masses are very irregular and much of the hme-silicate rock has formed at the expense of quartz monzonite, although perhaps most of it is of limestone derivation. The metamorphic minerals include pyroxene, garnet, vesuvianite, wollastonite, fluorite, quartz, and the metallic sulphides, chalcopyrite, pyrite, arsenopyrite, pyrrhotite, blende and galena. Cupriferous pyrite is the most important ore mineral. Careful study has revealed a definite sequence in mineral formation as follows :'2 1, aluminous pyroxenes; 2, aluminous garnet (grossularite) and vesuvianite ; 3, wollastonite ; 4, lime-iron pyroxene (hedenbergite) ; 5, lime-iron garnet (andradite) ; 6, fluorite, quartz and metallic sul- phides (and actinolite and hornblende) ; 7, metallic sulphides (and quartz and fluorite); 8, calcite. As the calcite is quite certainly residual from the limestone, it is clear that in the Dolores deposit the metallic sulphides were among the last metasomatic minerals developed and formed later than the lime-silicates. The paper above cited does not describe in detail the spacial relationship of the ore bodies to the limestone and monzonite, although it is stated that they ‘‘oceur largely at the very contact, frequently with limestone as one wall.’’!* In the paper by Prescott,’® however, sketches of the ore chimney at Dolores Mine, reproduced herein as figures 6 to 8, are pertinent. Figures 7 and 8 are clearly illustrative 12 Spurr, J. E., Garry, G. H., and Fenner, C. N., Study of a contact meta- morphic ore deposit: The Dolores Mine, at Matehuala, 8. L. P., Mexico, Econ. Geol., vol. 7, pp. 444-484, 1912. 13 [bid., p. 444. 14 [bid., p. 446. 15 Op. cit., p. 65. Potosi, Mexico. University of California Publications in Geology , v PP py tye Be ee eT aan VAY SA Ope Vy eh Ae Katy pt ype ee tA vevy VV Ye vt St Vpn Le OS vw hey ar UPPER HORIZON. Fig. 6 INTERMEDIATE HORIZON. Fig. 7 DEEP HORIZON. Fig. 8 CONTACT METAMORPHIC ROCK time Ll a [ Vou. 10 AVAIL MONZONITE|, /” ¥ VV) A, VS tA Generalized plans of ore chimney at Dolores Mine, Matehuala, San Luis After Basil Prescott, Econ. Geol., vol. 10, p. 65, 1915. 1916] Umpleby: Ore on the Limestone Side of Garnet Zones 33 of the occurrence of ore on the limestone side of garnet zones. The relations shown in figure 6 do not support the general idea, but it is introduced because it represents a part of the same chimney of ore shown in the other two figures and has value as a check to sweeping generalizations. Within the area represented by it the writer would expect to find clear evidence of replacement of the silicates by the sulphides. Mackay, Idaho.—The contact metamorphie copper deposits at Mackay, Idaho, occur well within a mass of granite porphyry which has invaded folded strata of Carboniferous age.1® Several engulfed blocks of limestone occur in the vicinity of the ore deposits and have been variously metamorphosed so that some are bordered by only a narrow margin of marble, others are more than half changed to lime- silicate rock, and still others are completely transformed to garnet- diopside rock and ore. Marmorization accompanied intrusion but the intense metasomatism followed the fracturing of a thick magma shell. In many places the granite porphyry bordering included lme- stone masses is extensively changed to garnet-diopside rock. The ore in the Copper Bullion Mine occurs along the margins of a block of limestone several hundred feet long and is separated from the granite porphyry by a zone of garnet-diopside rock from three or four to more than twenty-five feet wide. Marble forms the other wall, but this gives way within a few feet to normal limestone. The relations are illustrated in figure 9. The Alberta ore bodies, situated along a pronounced fault which traverses the igneous mass, comprise two groups of branching chimneys which occur in the central parts of large garnet areas (fig. 10). Here no central limestone body remains, and the occurrence is interpreted as representing the limiting stage of ore deposition on the limestone side of a garnet zone which surrounds an engulfed block. A study of the ores shows that the sulphides locally are contempo- raneous with the garnet crystals but that most of them are of distinetly later development. Whitehorse Copper Belt, Yukon.—The rocks of the Whitehorse district comprise Carboniferous limestone largely destroyed by three distinct igneous invasions, the principal of which, though of variable composition, is predominantly hornblende granite.’ The larger 16 Umpleby, J. B., The genesis of the Mackay Copper Deposits, Idaho, Keon. Geol., vol. 9, pp. 307-358, 1914. The ore deposits of the Mackay Region, Idaho, Prof. Paper, U. 8. Geol. Survey (in preparation). 17 McConnell, R. G., The Whitehorse Copper Belt, Yukon Territory, Can. Geol. Survey, No. 1050, 63 pp., 2 pls., 2 figs., 8 maps, 1909. [ Vou. 10 Geology ions in icat Publ nia versity of Califor nm U 34 ‘9U0Z JOUIVS B JO opis 9UOFSOUIT] Vy} UO e10 JO 9dUeIINDIO Sutmoys ‘oyepy ‘Aevyovy ‘Z ‘ON Jooyg uorfng 1teddop Fo suorjoes puv ue[q ‘6 “Siz 4901 JOueS > Ajpedioulig 4 e LA Ajpediouid A 3 VOM A . n ae Ny = z 4 7a) \ Nn G v ~ a = Sees Here 2 ay, ane Ne i RG es pene ype vs Askyduod ayiuve Sac u i £ : . ee a ee Se 2 ON Oe = ) ~ a i eS Vu we Fe e ‘ jouses pure. [sey ay Aky ~w “ =A = e WN ne vA 3 77 ’ Nv PEN, METH euo}sow sy 9Ad] QUUNY dAOgE GL : nats ra oie 4 eee Yyoouqoure aes 4 J8-8/NO ONY SaplUeIKy ey oe , ie 09 OF of 06 or ee ee ee ee | 4334 40 31V03 o 1916] Umopleby: Ore on the Limestone Side of Garnet Zones 35 ore-bodies occur in the limestone close to or adjoining the granite, but ore also occurs in the granite, ‘‘often at considerable distance from the limestone.’’ ‘‘The constituent minerals, and general character of the ore-bodies in the two formations, are very similar.’’ The principal copper minerals are bornite and chalcopyrite, which are associated either with magnetite and hematite or with garnet, augite and tremo- lite. ‘‘ All the ore-bodies of this (the latter) class, so far discovered, occur in the limestone, close to the granite, and are often separated from the granite by a zone of more or less completely replaced lime- NE a sf La Ks Eisai “Tengen et ieee “KLE “ley hite marble ° S90 1opo Feet Wy Ze Fig. 10. Section through Alberta Mine, Mackay, Idaho, showing occurrence of ore in the central part of a garnet-diopside mass. stone.’’'® This relationship is clearly brought out by the geologic maps of the Grafter Mine and the Best Chance ore-body. Endo- morphism has resulted in a considerable development of garnet, pyroxene and epidote in the granitic mass. INTERPRETATION The extent to which the occurrence of ore on the limestone side of garnet zones, as illustrated in the seven well known districts cited above, represents a general law cannot be definitely stated at present. Indeed, the object of this paper is merely to set it forth as a working hypothesis in the hope of arousing discussion and stimulating obser- vation. It is highly probable, however, that there are many more examples of the relationship. In papers on four of the districts cited one writer has clearly stated or illustrated the relationship, but in the writing of another on the same deposit I have been unable to find a quotable statement. The occurrence of ore on the limestone side of garnet zones, whether it be a constant relationship or not, must be explained for 18 Ibid., p. 22. 36 University of California Publications in Geology [ Vou. 10 the several important deposits cited above before knowledge of ore genesis approaches completeness. In the abstract there are two possible explanations; (1) either the sulphides form synchronously at a lower temperature than the lime-silicates and thus occur near the outer margin of metamorphism, or (2) the sulphide-rich solutions are delivered to the contact zone later than those characteristically forming lime-silicates, and replace the limestone in preference to the meta- morphic rock earlier developed. Probably most students of the subject will favor the latter view and in stong support of it is the occurrence of apparent feeders at Seven Devils which connect the ore downward across the garnet zone with the quartz diorite. Also in support of this alternative is the broad observation based on mineral paragenesis ‘that emanation of sulphides and magnetite continues after the con- tact action, resulting in silicate rock, is completed.’’ 1 But the alternative explanation must not be too ightly considered. If the sulphides form at lower temperatures than the lime-silicates, their zone of deposition may be expected gradually to draw in toward the source of energy as cooling of the intrusive mass progresses. This implies a superposition of minerals of lower temperature range upon those earlier formed at higher temperatures, providing that their source of supply is not earlier cut off or exhausted. Would not this give the same relations of sulphides to silicates as would a sequential supply of solutions of different type? It seems to the writer that the explanation of the phenomena requires broader considerations than the paragenetic relations of minerals in the hand specimen, although these have their value. It is generally recognized that the sulphides in part, perhaps in large part, develop contemporaneously with lime-silicates and that most of them occur in small amounts as constituents of igneous rocks. Thus, we would not expect to find a temperature control sufficiently marked to afford the relations observed in the deposits herein cited. The fact that the silicate minerals in most places are more widely distributed along the contact than the ore minerals is also probably significant.°° But the silicate minerals themselves are localized along the contact in many places and this has been considered as indicating the escape of the solutions through fissures in an outer magma shell.°? The par- 19 Lindgren, W., The origin of the ‘‘Garnet Zone’’ and associated ore deposits, Econ. Geol., vol. 9, pp. 283-292, 1914. 20 Lindgren, W., loc. cit., pp. 285-286. 21 Butler, B. S., Geology and ore deposits of the San Francisco and adjacent districts, Utah, Prof. Paper, U. 8. Geol. Survey, no. 80, p. 12, 1913. 1916] = Umpleby: Ore on the Limestone Side of Garnet Zones 37 ticular localization of the sulphide-bearing portions of the contact zones seem to be more rationally explained by solutions of different or gradually changing composition than by temperature control. SUMMARY AND CONCLUSIONS The preference of ore for the limestone side of seven important contact zones has been shown by citations and diagrams, and a desire has been expressed to ascertain through discussion how general this relationship is. The phenomena may be interpreted as due either to heat control or to a supply of solutions of changing composition such that lme- silicates are predominantly formed during the earlier stages of depo- sition and the sulphides during the later. The latter view is favored by the writer. If the relationship should prove to be a constant one it will be of considerable value in the exploitation of contact deposits, for other things being equal, development work will follow the limestone rather than the intrusive side of the garnet zone. Even at present enough is known to recommend that the habit of the individual deposit in this particular be carefully observed as a guide to later search for ore. In the case of engulfed blocks of limestone the limestone-side will in many places be the central part of the garnet mass. Transmitted May ft, 1916. ve ie ba veuuLeTiN, OF ‘THE DEPARTMENT oF GEOLOGY : Issued October 11, 1916 ‘AUNA OF THE FERNANDO OF > . LOS ANGELES BY CLARENCE L. MOODY eee Me UNIVERSITY OF CALIFORNIA PRESS BERKELEY | Nore. —The University of California. Publica i eations of learned societies and institutions, univers alll the publieations of the University will be sent upo publications and other information, address the Manager of the -—s«Gadifornia, U.S. A. Ali matter sent in exchange should be pe eerroeNy, University Library, Berkeley, ee U.S. A. eee OTTO HARRASSOWITZ R. 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MOODY CONTENTS PAGE ITT e150 CHIU CU Tages eee ge ae Seg necro re td Se Su cate sa teeaeesen= see et esdeso eee 39 (©) nag CIC Gece eerentens eee cee Mere are sour rere sar ey area gr SES Ser ee oe as ener nt 40 Previous knowledge-of related occurrences .............22..-2.---s2-0---ce--ceeceeeeecceeeceeeeeeeeee 40 LSBUSH CORE: SY XY ORCS) ee eer ee ee 42 BH) aT AS UTI Yin, ee eee oees eens yas Ses voces acne Subeen ence n sa seen ene cn Se eee 46 Generallteatures Of the fami ey: oeccecnces ccs ceeccecse sees cceensenceeeveceeee as -tcces nes ecdececeseeceseeeeesaee 46 Compas Onmwalltie nel ete uta Wis ever eee sees ceedeeeezesceveesceeeese ates ses eeeeceee tee ee so -caenssee eos 48 TOYSXSKOveT OW EAM CHa CoRe 4S) CXL SYS Ae re a ee eee ol Epitonium (Opalia) retiporosa Carpenter -.......0.00.20.20.220o2 eee ence 51 Siphon ayo Sits MSP se es ssa ss = seca en — ve eae see eee n= aan Sees Sta rcecee. ecu saee esses ts estates 51 (Clinmyyssroxslioneabis). orbits) seavenatobeiy ae \ eM ee ee eee eee 52 NTRS a aMay al ete piaatop ae Bt 1015) Oe ee eee see ee ere eee eee eee ree en ee ae eee 53 C(Oxortiaital oye Mey, Loxayasiees pal ialee hep a1 3h Oe eee seer ee ee RP ree ee 53 Turris (Drillia) modestus, n.sp. -...................-.-- eee ee oat ere 54 BOTS ONAN CUM ae MSY) s pereess ese sore cea neon waa fae ees eee eee dayne soe ese oes cee 54 Milam orilne simul CULC ay, TSP), 2aqcasecseseeceecesaceseeoeas CARL WIMAN fc i CONTENTS Ka ATATaNEeT50 CLITA ce © Tames tae se eee em cle ae er ce dr oe tee Sgt eae ee Ao ee oe 63™~ (ORT S) ee RS cD 63 IMixosaumusand sPhalarodom 22222-2222 scoececcceecccecee ee aaaeseeeeee--aeesese cceeeana-eseeccenencecessenseesee 65 eSSOSa@UEUS aNd SHAStASAUTUS) 2.22 .ee cece --2 eee eae - nose ee teee eee e aden ecenneee-neeescnseceeeserusenee 68 Ressopteny xsand. Omphalosaunus) 2. sescee-ce.c cece ceceee sec eee fect ceceeee ea ceceseeeeteeeeeceseeceeceeseeee 69 Hamas atlOM SLU S sesecescescc:ee- asec ste aceeccceecel ee et cease ete tees ieee. fbeen.deetbesesaccev toca dedncciees 71 NGAGE ALIN Cee eee eee, ee Rs PAP ae ee rete Rr On 73 INTRODUCTION It gives me great pleasure to comply with a request from two American colleagues to make a comparison between the marine Triassic reptiles of Spitzbergen and Europe on the one hand and western North America on the other, and I do this so much the more because on both sides a good deal has come to light since I treated the Triassic ich- thyosaurs from Spitzbergen in 1910.°°* Of reptiles, however, very little material has been added from the Trias of Spitzbergen since the saurian expedition in 1909. The expeditions of 1912 and 1913 have, like the one that is now in progress, been directed chiefly to the some- what older fish horizon with stegocephalians and fishes. OCCURRENCE Not very long ago the ichthyosaurians from the Trias belonged to the greatest rarities; now, on the contrary, they seem to be about * For literature references see bibliography forming the last division of this paper. Owing to uncertainty of transport during the past year it has not been possible for the author to read the proof of this paper.—Eprror. 64 University of Califorma Publications in Geology [ Vou. 10 equally rich in species, and at least in the northern hemisphere as widely distributed, as during the Jurassic. One knows of finds at a number of places in Germany, Switzerland, Italy, Austria, Rouma- ma,” England, Spitzbergen, arctic and western North America, and possibly New Zealand. Among these many finds there are, however, only a few that have given any, paleontologically, more enlightening material. The richest and most important have been the finds in the Daonella limestone, in the West Humboldt Range in Nevada, of Middle Triassic age; and in California, in the Hosselkus limestone, of Keuper age.'° The occurrence in northern Italy and Switzerland, just southeast of the southern extremity of Lake Lugano, generally known under the name of Besano, has been productive since the fourth decade of the nineteenth century, and was, though hardly yet fully appreciated, for a long time the only source of knowledge regarding the structure of the Triassic ichthyosaurians. These occurrences belong to a lower horizon of Keuper, Raibl-St. Cassian.* The German occurrences have hitherto yielded little, but recently a new find has been made, and the material seattered in various mu- seums has been brought together, so that von Huene’ has been able to show that twenty species, representing seven genera, are to be found. Of these, however, only eight species are sufficiently represented to make it possible for them to be named. Of the seven genera six are represented in other species from California, Nevada, Spitzbergen, and Besano. The whole of the material seems to come from the Muschelkalk. The Spitzbergen Trias vertebrates are, with a few exceptions, dis- tributed in four horizons. If the lowest, the first horizon, is fixed at zero, they lie at something like the following distances from each other : Mhe mew vertebrate WORTZ OM je -ceereec--ececceeee=s-ceveceee-reteee cen ere=a 360? m. AWAY qogay oYere (Spmub eee hal Valeeyial 0) 1 es eee ae a 205-210 The dower Saunlam MOrLZ OU) -eeccseceeressceesoe eee see eeeet ese ereeeee 93 BD Ere £15 eb by 0 12:71 0 Tn err te eee mean eS 0 With regard to stratigraphy in general, reference is made to the work by Nathorst.'® Above the arenaceous beds, belonging presum- ably to the Buntsandstein,** which were previously referred to the Permian, come the Posidonomya slates. Near the base of these lies the fish horizon, and somewhat deeper than that part of the layer which from older Swedish ammonite finds was known to Mojsisovies.” Probably the lower saurian horizon also comes within this layer. 1916] Wiman: Marine Triassic Reptile Fauna of Spitzbergen 65 The Posidonomya slates, as well as the following Daonella slates, with the upper saurian horizon, belong to the Muschelkalk. Above these bituminous slates again come arenaceous beds which, for the greater part at least, ought to represent the Keuper. Within these lies the new vertebrate horizon. The age relations of the better known Triassic ichthyosaurians thus becomes the following: To the Middle Triassic belong the finds in Germany, Nevada, and Spitzbergen, and to the Upper Triassic those in California and at Besano. MIXOSAURUS AND PHALARODON The genus Mixosaurus was erected by G. Baur’ in 1887, and was founded on the Lombardy species M. cornalianus Bass., which now, by the researches of Repossi'S and myself,?’ is pretty well known. In 1891 E. Fraas’ incorporated with this genus, under the name Jch- thyosaurus atavus, the species originally described by Quenstedt.'* This procedure was accounted for by I. atavus having elongated fore- arm bones, sparse and dimorphous teeth, ete., characters which one now knows are peculiar to Triassic ichthyosaurians in general, and therefore cannot be used as generic characters. For the same reason Dames® took this view. Judging by the little hitherto known of I. atavus, it cannot belong to the genus Mixrosaurus. For still less important reasons Dames referred to the genus Mviro- saurus the smaller of the only two species from the Spitzbergen Triassic. This, however, has turned out more successful, and new material having been added since 1909, I did not hesitate, in 1910, to class Mixosaurus nordenskioldi with this genus. In this view I have been further strengthened since I succeeded in obtaining material of the Besano species and studied Repossi’s original specimens in Milan. In 1910 a work by Merriam” was published in which a new species, Phalarodon fraasi, was described. It then appeared that I had prob- ably made a mistake, in so far as I had also classed the Phalarodon- hke jaw fragments with Mixosaurus nordenskioldi (1910, pl. 5, figs. 10, 12, and 13). In so doing I conceived the possibility of a difference in sex of such a nature that the less pronounced dimorphous teeth might represent, for example, young females and the more developed dimorphous teeth old males. My figure 10 shows a transition, on the one hand, from those which I still wish to class with Mixrosaurus nordenskioldi (figs. 9 and 11) and the perfectly Phalarodon-like ones in figures 12 and 13. 66 University of California Publications in Geology [ Vox. 10 In his work of 1911 Merriam?’ called attention to the similarity between Phalarodon and certain of my specimens, and I now consider it probable that the jaw fragments (pl. 5, figs. 12 and 13) at least, are to be connected with Phalarcdon, which is a special type. After having seen comprehensive material of Mirosaurus cornalianus, I have found that the appearance of the teeth is very constant in different specimens, and from investigations by Dollo* of the mosasaurian Globidens fraasi, in which also Phalarodon is treated, it has also be- come probable that the posterior teeth of Phalarodon indicate a very diverging diet. As, however, there is in the grade of dimorphism of the teeth a very even transition from M. cornalianus over M. norden- shioldi and to the pronounced Phalarodon type, one ought perhaps to await a more complete knowledge of the crania of the Mirosaurus species, and new discoveries of remains of Phalarodon, of which hitherto only cranium parts are known, before one decides where the boundary between Mirosaurus and Phalarodon should be fixed, and whether the difference really is so great that it warrants the setting up of a new genus. For the present I will, therefore, keep M. corna- lianus and M. nordenskioldi together within the same genus. To it belongs, with a certain degree of possibility, also Cymbospondylus? natans Merriam from Nevada. The anterior limb indicates, as will be seen by the accompanying figures (figs. 1 and 2), great similarity, especially to the species from Spitzbergen. The piece of the vertebral column, which Merriam classes with this species, does not contradict this supposition. It is perhaps not excluded that Phalarodon fraasi is the cranium of this species, for it originates from the same horizon. The pelvie arch of M. nordenskioldi is, as I have previously shown, almost identical with that of M. cornalianus, which has also a foramen pubicum. As Merriam has rightly observed from my figure of the vertebral column, a portion of the tail is missing, but it is seen from loose vertebrae that the tail has not narrowed off suddenly, as with the whales, but very slowly, as with other ichthyosaurians. The part of the tail that lay behind the caudal fin must therefore have been very long. Merriam also conceives of the possibility of my having placed the pelvis too far back. This I do not consider probable, for I am very sure about the position of the pelvis. The difficulties that Mer- riam finds in the, with all this connected, placing of the caudal fin disappears if one takes another view of the origin of the caudal fin than Merriam. I have imagined that the caudal fin is a dorsal fin, 1916] = Wiman: Marine Triassic Reptile Fauna of Spitzbergen 67 which moves backwards, and first during the Jura period reaches the tip of the tail, where it becomes stationary, after which the portion of the vertebral column located within the fin begins to shrink. In this view of mine I have also been strengthened by Fraas”® deseription of the remains of a very young specimen of /chthyosaurus quadri- scissus Quenst., which in this respect constitutes something between, for instance, Mirosaurus nordenskioldi and the full-grown J. quadri- és if Fig. 1—Miaosaurus? natans Mer- Fig. 2.—Mixosaurus nordenskioldi riam. Anterior limb, X % (combined Hulke. Anterior limb, XK % (after after Merriam and partly restored). Wiman). H, humerus; R, radius; U, ulna. scissus. It then also becomes perfectly natural that the fin-defining downward bend of the tail in the older Middle Triassic W. norden- skioldi, lies more forward than in the younger Upper Triassic J. cornalianus, In which the fin ought to have had time to move a little farther back. In Cymbospondylus petrinus, also Middle Triassie, the tail-curve hes, according to Merriam, still farther baek than in the younger M. cornalianus. This, however, need prove nothing more than that in another quite different tribe of ichthyosaurs the move- 68 University of California Publications in Geology [ VoL. 10 ment of the caudal fin took place at a quicker pace than in the mixosaurians. PESSOSAURUS AND SHASTASAURUS Of the material from the upper saurian horizon of Spitzbergen, which I have tried to unite with Pessosaurus polaris Hulke, only the coracoid, humerus, radius, ulna and a few podial bones are found to- S 3 Fig. 3.—Shastasaurus osmonti Mer- Fig. 4.—Pessosaurus polaris Hulke. riam. Anterior limb, x 14 (after Anterior limb, X 4. Merriam). C, coracoid; H, humerus; R&, radius; U, ulna; J, intermedium; 7, trochanter. gether. As the ulna was destroyed in the preparation, I have not figured it before, although a very important fragment in juxtaposition to the radius is left. The bone had, however, the shape, very nearly at least, that I have reproduced in the accompanying figures (figs. 3 and 4). This neglect on my part has doubtless contributed to the peculiarities of the species, over against Shastasaurus, not having ap- peared as clearly as could have been desired. A comparison between 1916] Wiman: Marine Triassic Reptile Fauna of Spitzbergen 69 the figures of Pessosaurus polaris Hulke and Shastasaurus osmonti Merriam proves that quite another type is before us. The coracoid undeniably shows a certain likeness to the same bone in Shastasaurus, but it is more elongated longitudinally, which, however, is of little importance. This type of humerus differs widely from all the Amer- ican species and recurs only in Pessopteryx, the species of which, one and all, possess this thick, round type. Also radius and ulna have an appearance diverging very much from all other forms, caused by their belonging to a species with short, broad fins, within which the dis- placement of the bones has proceeded farther than with any other Triassic ichthyosaurian. For though the, for all such typical remain- ing portion of the forearm, elongation still is marked by the round not eartilage-filled hole between the radius and the ulna, the intermedium has pressed in just as far between the forearm bones as, for instance, in the Jurassic [chthyosaurus communis Conyb. The fore limb of Pessosaurus thus shows arrangement and form of the bones quite different from the corresponding characters in Shastasaurus. PESSOPTERYX AND OMPHALOSAURUS The material from the Lower Saurian horizon of Spitzbergen is very difficult to handle, as it consists of mere loose bones and bone fragments which le seattered on the float soil. Most of the bones are present in a very great number of specimens, and I still consider it probable that the majority belong to an ichthyosaurian which I have called Pessopteryx nissert. In addition, some smaller species chiefly of the same time must be present. To Pessopteryx nisseri I also referred, by way of proposal, and with much hesitation, a large number of jaw fragments with queer, button-like teeth in several rows. When I referred these teeth to an ichthyosaurian I imagined a change of diet something hke the one that has now really been verified in Phalarodon and Globidens. That the teeth were set in several rows I imagined to be due to the fact that, for the greater part at least, they consisted of reserve teeth, not yet used, which in that case ought to be arranged much the same as with the crocodiles, although, as far as I have yet been able to ascertain, they lie wholly embedded in the bone substance. Resorption of bone substance is of course nothing unusual in connection with displace- ment of teeth and horny cases, and also the embryological origin of similar teeth ought to be histologically possible. 70 University of California Publications in Geology [ Vor. 10 These jaw fragments now seem to me to be somewhat less enig- matical, since Merriam has pointed out that they do not belong to an Ichthyosaurian. In 1906 Merriam’ deseribed a reptile, widely dif- ferent from the ichthyosaurians but with a still uncertain systematic position, Omphalosaurus. It is found in the Middle Triassic of Nevada, and is thus approximately in the same horizon as Pessopteryz. The reproductions of the teeth of Omphalosaurus that are found in this work did not suggest to me any thought of the enigmatical teeth of Spitzbergen. Merriam, however, in 1911,1° has shown the great similarity between the Omphalosaurus teeth and the teeth referred by me to Pessopteryx, and since Merriam and Bryant" the same year produced new figures of Omphalosaurus teeth I ean inyself Fig. 5—Phalanges from the Lower Saurian horizon on Spitzbergen, X % (after Wiman). state the identity. But seeing that the teeth are identical, in what relation do then Omphalosaurus and Pessoptery. stand to each other ? Of the former only parts of the cranium with teeth and biconcave, ichthyosaur-lke cervical vertebrae are known, and, again, of the latter vertebrae, extremity and girdle bones are found. Therefore a com- parison cannot be made. One can, however, think of two possibilities. The one is, that all of the material represents Omphalosaurus. Mer- rlam seems to be inelined to this interpretation. One would then have to imagine a reptile with a relatively short head and a body that in detail had developed on the same line as Ichthyosaurus. Such a paral- lelism is of course not inconceivable, but less probable. The other probability is that an ichthyosaurian Pessopteryx is before us, but that, together with its bones, jaw fragments of Omphalosaurus oceur. It is easily possible that these very jaw bones have constituted the most lasting part of the skeleton. In favor of a foreign intermixture also speaks the fact that together with the Pessopteryx bones occur very 1916] =Wiman: Marine Triassic Reptile Fauna of Spitzbergen (0 numerous phalanx-like bones of different length, which, as I have pre- viously pointed out, cannot be located in an ichthyosaurian skeleton, but which might possibly belong to the Omphalosaurus teeth. That an ichthyosaurian Pessopteryx should develop a peculiarly formed humerus, which is identically like that of another ichthyosaurian, Pessosaurus, from the same region, is by far not so strange as that a reptile of an altogether different tribe, Omphalosaurus, should acquire just this humerus type. I therefore consider the probability larger that in addition to Pessopteryx nisseri also a representative of the genus Omphalosaurus is before us. FAUNAL RELATIONSHIPS I ean therefore agree with Merriam that the marine Triassic saurians of Spitzbergen and of central and southern Europe show a noticeable similarity with those of the Triassic of North America. The Mirosaurus species nordenskioldi, cornalianus, and natans are undoubtedly nearly related. If, then, a separate genus, Phalaradon, be added, common to Spitzbergen and western North America, this of course increases the similarity. Judging by von Huene’s previous communications, a number of American ichthyosaurian genera are also to be found in the middle European Muschelkalk. Omphalosaurus, wherever it belongs, is also a genus common to Spitzbergen and North America. If, however, important similarities exist between the Triassic marine saurians in the Old and the New World, there are also greater dis- similarities. These differences appear among the ichthyosaurians. In western North America are found numerous species of the genera Cymbospondylus, Toretocnemus, Merriamia, Delphinosaurus, and Shastasaurus, which do not appear in Europe or Spitzbergen. The Central European Muschelkalk no doubt also contains one or two specific types, and Pessosaurus and Pessopteryx are characteristic of Spitzbergen. If we turn to other reptile groups that are not adapted to a pelagic mode of living in such a high degree as the ichthyosaurians the dis- similarities of course become greater. In the Alpine Trias two notho- saurians, Pachypleura (Neusticosaurus) from Besano and the some- what younger Lariosaurus of Perledo, are found. In the Middle Euro- pean Muschelkalk are found numerous nothosaurians and placodonts. The marine Trias beds in Spitzbergen also contain several evidently 12 University of California Publications in Geology [ Vou. 10 marine labyrinthodonts,?? and in western North America are found thalattosaurians*!! to which one nowhere has found any analogy. Lastly, I would like to draw attention to a hitherto utterly neg- lected region containing marine Triassic saurians, namely, Arctic North America, where we have long known that ichthyosaurians are to be found. Triassic beds le exposed on Prince Patrick Island, Parry Islands, and on the western side of Ellesmere Land. One or more of these islands could, no doubt, be reached by ship, at least during favorable years, and from the eastern parts collections could be freighted down on sledges across Ellesmere Land, to the eastern shore of which one can come with ships by Smith Sound. How accessible the occurrences on either side of the northern part of Smith Sound are I do not know. Transmitted February 25, 1916. 1916] Wiman: Marine Triassic Reptile Fauna of Spitzbergen as LITERATURE 1. Alessandri, G. De, Studii sui pesci triasici della Lombardia. Mem. Soe. Ital. di Sci. Nat., vol. 7, fase. 1, Pavia, 1910. . Baur, G., Ueber den Ursprung der Extremitiiten der Ichthyopterygier. Be- richt d. oberrhein. geol. Ver., 20 Verslg., 1887. 3. Dames, W., Ueber die Ichthyopterygier der Triasformation. Sitzungsber. Akad. Berlin, Jahrg. 1895, Bd. 2, p. 1045, Berlin, 1895. 4. Dollo, L., Globidens Fraasi. Arch. de Biol., vol. 28, p. 609, Liege, 1913. 5. Fraas, E., Die Ichthyosaurier der siiddeutschen Trias- und Jura-Ablagerungen. Verlag der H. Laupp’schen Buehh., Tubingen, 1591. 6. Fraas, E., Embryonaler Ichthyosaurus mit Hautbekleidung. Jahresber. d. Ver. vaterl. Naturk. in Wirttemberg, Jahrg. 1911, p. 480, Stuttgart, 1911. 7. Huene, F. v., Iechthyosaurier der schwabischen Trias. Vortrag. Ibid., Jahrg. 70, 1914. 8. Merriam, J. C., The thalattosauria.. Mem. Calif. Aead. Se., vol. 5, no. 1, 1905. 9. Merriam, J. C., Preliminary note on a new marine reptile from the middle Triassic of Nevada. Univ. Calif. Publ. Bull. Dept. Geol., vol. 5, no. 5, p. 75, Berkeley, 1906. 10. Merriam, J. C., Triassic ichthyosauria with special reference to the American forms. Mem. Univ. Calif., vol. 1, no. 1, Berkeley, 1908. 11. Merriam, J. C., Notes on the osteology of the thalattosaurian genus Nectosaurus. Univ. Calif. Publ. Bull. Dept. Geol., vol. 5, no. 13, p. 217, Berkeley, 1908. 12. Merriam, J. C., The skull and dentition of a primitive ichthyosaurian from the Middle Triassic. Jbid., no. 24, p. 381, Berkeley, 1910. 13. Merriam, J. C., Notes on the relationships of the marine fauna described from the Triassic of Spitzbergen by Wiman. [bid., vol. 6, no. 13, p. 317, Berkeley, 1911. 14. Merriam, J. C., and Bryant, H. C., Notes on the dentition of Omphalosaurus. Ibid., no. 14, p. 329, Berkeley, 1911. 15. Mojsisovies, E., Arktische Triasfaunen. Mém. Acad. Imp. Se. St. Pétersb., ser. 7, tom. 33, no. 6, St. Petersburg, 1886. 16. Nathorst, A. G., Beitrige zur Geologie der Biren-Insel, Spitzbergens und des Konig-Karl-Landes. Bull. Geol. Inst. Upsala, vol. 10, p. 261, Upsala, 1910. 17. Quenstedt, Fr. A., Handbuch der Petrefactenkunde. 1852. 18. Repossi, E., Il Mixosauro degli strati Triasici di Besano in Lombardia. Atti Soe. Ital. di Se. Nat., vol. 14, Milano, 1901. 19. Simionescu, I., Ichthyosaurierreste aus der Trias von Dobrogea (Rumianien). Bull. Sect. Sci. de 1’Acad. Roum., année 1, no. 2, p. 81, Buecarest, 1913. 20. Wiman, C., Ichthyosaurier aus der Trias Spitzbergens. Bull. Geol. Inst. Upsala, vol. 10, p. 124, Upsala, 1910. 21. Wiman, C., Ueber Mixosaurus cornalianus. IJbid., vol. 11, p. 250, Upsala, 1912. bo 22. Wiman, C., Ueber die Stegocephalen aus der Trias Spitzbergens. Ibid., vol. 13, p. 1, Upsala, 1914. 23. Wittenburg, P. v., Ueber Werfener-Schichten von Spitzbergen. Bull. Acad. Imp. Se. de St. Pétersb., Jahrg. 1912, p. 947, St. Petersburg, 1912. ‘MAMMALIAN FAUNAS FROM MIOCENE DIMENTS NEAR TEHACHAPI PASS IN THE SOUTHERN SIERRA NEVADA \ ( BY ion ae JOHN P. BUWALDA y, UNIVERSITY OF CALIFORNIA PRESS BERKELEY UNIVERSITY OF _ Nore.—The University of California P eations of learned societies and ‘institutions, un i all the publications of the University will be sent upon publications and other information, address the Manager Univer Pr California, U. S. A. All matter sent in exchange should be Aun hs to Tt e Department, University Library, Berkeley, California, U. s. OTTO HARRASSOWITZ R. pideor amine LEIPZIG ‘BERLIN — Agent for the series in American Arch- ; Agent for the series in Ar aeology and Ethnology, Classical Philology, - aeology and Ethnology, Agricultu: Economics, Education, History, Modern Botany, Geology, Mathematics, E Philology, Philosophy, Psychology. Physiology, Zoology, and Memoirs. Geology. ANDREW C. Lawson and JoHN C. MeRRIAM, Editors. Price, volumes 1— -1, volumes 8 and following, $5.00. Cited as Univ. Calif. Publ. Bull. Dept. Geol. Volume 1, 1893-1896, 435 pp., with 18 plates, price LG Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price ..... Volume 3, 1902-1904, 482 pp., with 51 plates, Price .....--ssc:o:scteccsesessnsesesneeeeesee Volume 4, 1905-1906, 478 pp., with 51 plates, price ‘ . Volume 5, 1906-1910, 458 pp., with 42 plates, price A list of titles in volumes 1 to 5 will be sent upon request. _ VOLUME 6. \ . The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller : aft . Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern ¥ Nevada, by John C. Merriam. Part I.—Geologie History , The Geology ‘of the Sargent Oil Field, by William F. Jones Additions to the Avifauna of the Pleistocene Deposits at Fossil Lake, Oregon, Br Looye ‘Holmes: Miller 2.022.200 ticsc2p-seeecbecpoct bene duececectietoczedeetesencuenasseteng soos er 5. The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Reid 6. Note on a Gigantic Bear from the Pleistocene of Rancho La Brea, by John C. Merriam. rd A Collection of Mammalian Remains from Tertiary Beds on the Mohave Desert, by John C. Merriam. Noss 6 and \\7. imvome (eG vera srr ee ean ccc cet cactra-nacst ee See Dee eee eS 8. The Stratigraphic and Faunal Relations of the Martinez Formation to the Chico and Tejon North of. Mount Diablo, by Roy H. Dickerson -.....0..2.222-ctcsscecsettecneeesne z 9. Neocolemanite, a Variety of Colemanite, and Howlite from Lang, Los ‘Angeles County, California, by Arthur 8S. Hakle 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. Taylor... 11. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern Nevada, by John C, Merriam. Part II.—Vertebrate Faunas 12. A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, by Loye Holmes” MWiller® 2 oone2s.cccccess ace cesnecnteecennecnnenarbgendpoceuntoasingenest ncn conantacee ites rues sean dacedeet tee 13. Notes on the Relationships of the Marine Saurian Fauna Described from the Triassic of Spitzbergen by Wiman, by John C: Merriam. 14. Notes on the Dentition of Omphalosaurus, by John C. Merriam and Harold C. Bryant. pe po oH Nos, 13 and 14 in one! cover ......ics:--26--- 0b itge eee Be 15. Notes on the Later Cenozoic History of the Mohave Desert Region in Southeastern California, by Charles Laurence Baker .......2cc.: 2coeceossssesnsapsnsecencpuesssesen2s eee . 50e 16. Avifauna of the Pleistocene Cave Deposits of California, by Loye Holmes Miller 17. A Fossil Beaver from the Kettleman Hills, California, by Louise Kellogg ........ 18. Notes on the Genus Desmostylus of Marsh, by John C, Merriam ...................- 19. The Elastic-Rebound Theory. of Earthquakes, by Harry Fielding Reid .............. VOLUME 7. Beene 1, The Minerals of Tonopah, Nevada, by Arthur S. Eakle ....---cc-ccecccccecccsceccccceensoes 2. Pseudostratification in Santa Barbara County, California, by George Davis Loud Dak” qu. chan-cacdeadeensed-teascputat leececsatogs othe han seedptee dst oase een chendins ate, pay Sn ee 3. Recent Discoveries of Carnivora in the Pleistocene of Rancho La Brea, by John | ! Merriam acnceczccengeehcenns te ctec eres ec eree eee, eae ee ee a 4. The Neocene Section at Kirker Pass on the North Side of Mount Diablo, Tog Car ke. \opcs.. sacs -desasioanedpcepdeceonece epee teste tee sos Peta eee ES . Contributions to Avian Palaeontology from the Pacific Coast of North Amerie; Loye Holmes Miller OU UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 6, pp. 75-85 Issued November 18, 1916 NEW MAMMALIAN FAUNAS FROM MIOCENE SEDIMENTS NEAR TEHACHAPI PASS IN THE SOUTHERN SIERRA NEVADA \ OS JOHN P. BUWALDA ry NN, Cry P CONTENTS " PAGE MTG NO CU G1 OM Yee a oes 2s Sessa a rece e eese eee oe ee eee Se ce Sei nee ere eee re 75 (QN CEU EN ILS Seer ae Pee 76 ey seam Chi Haan a eee essence ee nete sees seceie eensseeeectecectecetee sees poo saneeaeentes tid esses 77 (Cel race), LEYS 1 EDF pee a em eee re 80 TRE) EER EG VaNV A ofp ee 5) 1 FEE EK) zeae PP 81 Geologie Significance of the Faumas —........2...2..22..22.222.-200cseeecee cess ee ee ee eee .. 84 INTRODUCTION During the past five years expeditions under the direction of the Department of Palaeontology of the University of California have made considerable collections of Tertiary mammalian fossils in for- mations near Barstow and at Ricardo, in the Mojave Desert. Mam- malian material has also been obtained in sections containing marine formations in the Southern San Joaquin Valley, on the western or opposite side of the southern Sierra Nevada. Study of this material from the Mojave Desert and the San Joaquin Valley has yielded important information regarding the history of mammalian life in these regions. With the geologic data obtained it is being made the basis for a beginning in the correlation of events in the Tertiary palaeontologic and geologic history of the Great Basin and Pacific Coast provinces. With a view to contributing to the solution of this general problem of Cenozoic correlation between the Great Basin and Pacifie Coast ae ie Y '™ 5 iy eat nea oe Sepa JOHN C. MERRIAM m JAN J- 195i Le B we a ayy * 4 Fs Sele +t ~ Oy : Oral Masi “ us REMAINS FROM A LATE TERTIARY FORMATION AT IRONSIDE, OREGON f “ } ieee : * Asin BY . _ JOHN C. MERRIAM Z A ees aA Si 7 a p f re ‘ “A "¢ 2 UNIVERSITY OF CALIFORNIA PRESS : > _ BERKELEY ie eye Pee belt publications and other information, address the Manager California, U. S. A. All matter sent in exchange shoul - Department, University Library, Berkeley, Cat oni. U.S. . ‘Nore.—The University of ‘Dalitonnrd Pul : eations of learned societies and institutions, A OTTO HARRASSOWITZ R.. FRIEDLAENDER | c LEIPziI¢ es BERLIN: Agent, for the series in American Arch- Agent for the series i r aeology and Ethnology, Classical Philology, aeology and Ethnology, Agricu lesa Ie Economics, Education, History, Modern Botany, Geology, Mathematics, Patho Philology, Philosophy, Psychology. Physiology, Zoology, and Mem TS. Geology.— ANDREW C. Lawson and JouN C, MERRIAM, Beis Eee volumes _ an = or . The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Rei . Note on a Gigantie Bear from the Pleistocene of Rancho La nee by John C. . The Stratigraphic and Faunal Relations of the Martinez Formation to ‘the. . Neocolemanite, a Variety of Colemanite, and Howlite from Lang,’ Los Ang es . A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. Taylor... . Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Newiyet n . A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, by Loye Holmes . Notes on the Relationships of the Marine Saurian Fauna Deseribed from the Te assic . Notes on the Dentition of Omphalosaurus, by John OC. Merriam and Harold C Bryant, . Notes on the Later Cenozoic History of the Mohave Desert Region in Southeastern — : . Avifauna of the Pleistocene Cave Deposits of California, by Loye Holmes Miller... 1 . A Fossil Beaver from the Kettleman Hills, California, by Louise ee ai ag . Notes on the Genus Desmostylus of Marsh, by John C. Merriam ............. . The Elastic-Rebound Theory of Earthquakes, by Harry Fielding Rei . The Minerals of Tonopah, Nevada, by Arthur S. Bakle ................. . Pseudostratification in Santa Barbara County, California, by George . The Neocene Section at Kirker Pass on the North Side of Mount Diavleg cer B . Contributions to Avian Palaeontology from the volumes 8 and following, $5.00. : Cited as Univ. Calif. Publ. Bull. Dept. Geol. Me fet Volume 1, 1893-1896, 435 pp., with 18 plates, price = Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, pre Volume 3, 1902-1904, 482 pp., with 51 plates, price ................-- Volume 4, 1905-1906, 478 pp., with 51 plates, price .......... Volume 5, 1906-1910, 458 pp., with 42 plates, price ...........------:-0----- sees A list of titles in volumes 1 to 5 will be sent upon request. VOLUME 6. . The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller........... . Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Nevada, by John C. Merriam. Part I.—Geologie History................-.. The Geology of the Sargent Oil Field, by William F. Jones .............. f Additions to the Avifauna of the Pleistocene Deposits at Fossil Lake, Oregon, by Loye Holmes Miller Merriam. a by John C. Merriam. Nos, 6 and”7 in ONG@. COVED) 1. ..2::---ti-cceseseensncsasednosecte=rcaccesth soa neentesbsnease eee ee and Tejon North of Mount Diablo, by Roy HE. Dickerson ..............-.:-2:-. ee Ameghino, F., Notas sobre una pequefa coleccion de huesos de mamiferos procedentes de las grutas caleAreas de Iporanga en el Estado de Sao Paulo- Brazil, Revista do Museu Paulista, vol. 7, pp. 74-119, 1907. 6 Sinclair, W. J., New mammalia from the quaternary caves of California, Univ. Calif. Publ. Bull. Dept. Geol., vol. 4, pp. 153-155, pl. 23, figs. 15a and 8, 1905, 7In a discussion of the quicksilver deposits of the Terlingua district, Brewster County, Texas, H. W. Turner makes mention (Hconomie Geology, vol. 1, p. 275, 1906) of the finding of ground-sloth remains in a fissure deposit. This material was submitted to Professor J. C. Merriam, who identified several teeth as belonging to Nothrotherium. The specimens were placed in the Museum of the California Academy of Sciences in San Francisco, where they were destroyed by the fire of April 18, 1906. Recently O. P. Hay has described (Proc. U. S. Nat. Mus., vol. 51, pp. 116-123, pls. 6 and 7, 1916) a new species, Nothrotherium texanum, from the Pleistocene of Texas. 1917 | Stock: Skull and Dentition of Nothrotheriwm 139 Museum of History, Science and Art of Los Angeles. For the privilege of studying this remarkable collection of nothrotheres, I am very greatly indebted to Director Frank 8. Daggett. Thanks are due also to the other members of the Museum staff for many courtesies extended. I am obligated to Professor John C. Merriam for assistance and much friendly advice and eriticism during the progress of the research on the Rancho La Brea edentates. The drawings reproduced in this paper have been prepared by Mrs. Louise Nash. CRANIUM The largest available skull of Nothrotheriwm from Rancho La Brea is approximately as long as a skull of Megalonyx jeffersoni described Fig. 1. Nothrotherium shastense Sinelair. Cranium, no. 208 M. TH. S. A., superior view, X 144%. Rancho La Brea Beds, California. by Leidy.* With this exception the specimens from the asphalt beds are all somewhat shorter than either M. jeffersoni or M. leidyi. In marked contrast to Megalonyx, however, is the relative slenderness of skull in Nothrotherium. Yn this respect the latter genus more closely resembles the Miocene Megalonychidae and Planopsidae,® from which it has also deviated less than Megalonyx in general shape of skull. Contrasted with Planops, one of the largest of the Santa Cruz Gravi- grada, the skull of the Pleistocene genus is distinctly larger. 8 Leidy, J.. A memoir on the extinct sloth tribe of North America, Smithson. Contrib. Knowl., vol. 7, 1855; see measurements of the Dickeson specimen, p. 13. 9 Scott, W. B., Rept. Prin. Univ. Exp. Patag., 1896-1899, vol. 5, p. 164, fig. 16, 1903. 140 University of California Publications in Geology [ Vou. 10 Nothrotherium differs from Megalonyx and agrees with Hapalops in the long and slender muzzle (fig. 1). In no. 632'° the anterior ends of the maxillaries are noticeably flared. This character is less appar- ent in no. 633 and may be but little developed as in no. 634. The nasals are long and may be more decidedly arched in some skulls than in others. In no. 632 the fronto-nasal suture is convex posteriorly, thus resembling most species of Hapalops. This suture may, however, vary in Nothrotherium. It may be decidedly V-shaped as in no. 633, but in this specimen the original suture appears to have been some- what in advance of the present separation. In no. 633 the nasals have apparently fused with the frontals, a secondary or pseudo fronto- nasal suture developing posterior to the original suture. An extensive inflation of the pterygoid in skulls of the tree sloths Choloepus and Hemibradypus has been noted by Anthony.?® With reference to the air sinuses in the skull of the former genus, he states: Le sinus sphénoidal s’étend latéralement a 1|’intérieur des ptérygoides, se prolonge dans le temporal, envahissant la base de l’apophyse zygomatique et venant presque au contact des prolongements latéraux du sinus frontal. Le crane osseux présente un orifice situé 4 la face interne et antérieure de chaque ptérygoide et qui conduit dans ce sinus.27 Nothrotherium therefore resembles Choloepus very closely not only in the large size of the pterygoid inflation but also in the presence of an orifice perforating the inner wall of the pterygoid. The alisphenoid forms not only the roof of the pterygoid bulla but the dorso-internal wall as well. In some skulls an internal continua- tion of the vacuity of the pterygoid extends toward the middle line. In skull 634 this extension, lying below the ventral surface of the basisphenoid, is separated from its fellow of the opposite side by a median partition only 2mm. in thickness. The development of these internal sinuses varies from the extreme case seen in no. 634 to their entire absence as in skull 15. The basisphenoid is concave transversely and tapers towards the anterior end where the pterygoid bullae approach each other most closely. The basioccipital in most skulls is short, relatively much more so than in Megalonys. The tympanic, as seen in no. 208, resembles Hapalops in the incomplete, irregular circle of bone which encloses ventrally the large external auditory meatus. Anteriorly the tympanic may touch the dilated wall of the pterygoid. Posterior to the tympanic is the stylo-hyal process with its ovoid depression. It is situated much closer to the occipital condyle than in Megalonyz. The small condylar foramen hes in a pit and may be entirely hidden by the border of the occipital condyle. In Hapalops and especially in Megalonyx this foramen is well in front of the occipital condyle. The paroccipital process, as in Hapalops, is inconspicuous, being much less prominent than in Megalonyx. Between it and the stylo- 25 Lindahl, J., Description of a skull of Megalonyx leidyi, n.sp., Trans. Amer. Philos. Soe., vol. 17, n.s., p. 7, 1893. 26 Anthony, R., Recherches anatomiques sur les bradypes arboricoles, etc., Ann. Sci. Nat., ser. 9 (Zool.), vol. 9, pp. 157-285, pls. 2-6, 1909. 27 Anthony, R., ibid., p. 178, 1909. 1917] Stock: Skull and Dentition of Nothrothertum 147 hyal process is a deep groove which reaches the occiput and extends for a short way along its lateral border. The position of the occipital condyles with reference to the pterygoid bullae has already been noted. The condyles in ventral aspect are not obliquely placed as in Megalonyx, and project posteriorly much less than in that genus or in Megatheriwm. They may be widely separated as in no. 313, or much closer together as in no. 203. By far the greater articulating surface of the condyles is directed downward, forward and outward. Leidy states that in Megalonyx the articulating surface of the condyles is bent at about the middle. In no. 633 the dorsal portion of the outer border of the condyle is curiously flattened by a rough and rather extensive surface. The foramen magnum may be transversely oval in shape. It opens more downward than in Megalony.r. The base of the zygoma is long, and the glenoid fossa is somewhat concave transversely. The zygomatic process is quite lke that in Fig. 4. Nothrotherium shastense Sinclair, Cranium, no. 208 M. H. 8, A,, posterior view, X 1%. Rancho La Brea Beds, California. Hapalops, differing from Megalonyx in not projecting so far from the side of the skull. As in Miocene genera, the occiput of the Rancho La Brea Nothro- therium is nearly vertical or inclined slightly beyond the occipital condyles. The supraoccipital forms usually an extensive, forwardly inclined surface. In posterior view (fig. 4) the condyles are seen to be as a rule more widely separated than in Hapalops. In no. 203 their position is more as in the latter genus. The posterior face of the condyles is relatively smaller than in Hapalops. The dorsal lip of the foramen magnum is notched at the middle only in skulls 15 and 166. The median vertical ridge of the occiput does not usually reach the foramen magnum. It is sharp below but greatly broadens dorsally on the surface of the supraoccipital. Where the vertical surface of the occiput meets the forwardly inclined surface a heavy, rugose, trans- 148 Umversity of California Publications in Geology verse ridge is formed as in Megalonyz. [ Vou. 10 This ridge swings outward and downward and in some skulls is directly connected with the pos- terior surface of the stylohyal process. not prominent except along its lower end. MEASUREMENTS OF CRANIUM Length from anterior end of maxillaries to posterior end of occipital condyles.......... Length from anterior end of nasals to pos- No. 166 M.H.S. A. Rancho La Brea N. shastense terior end of supraoccipital ...................- 339.8 Length of palate, from anterior end of maxillaries to postpalatine notch -........... 141.7 Jreatest width of palate anterior to M2?...... 45.8 Width of palate between alveoli of M#........ 22 Greatest width of pterygoid bulla -............. 41.4 Greatest length of internal orifice of ptery- FRG) GOA LD ULL] era meereer oe nena on Pee nee ete sunseace 37.6 Greatest width of internal orifice of ptery- ond | WOU a soso sae ese ste eccccsasecctescacsaestecees? useceast Least distance between pterygoid bullae... ........ Mastoid width above stylohyal processes ..... 112.8 Greatest width across occipital condyles... 75.4 Transverse diameter of foramen magnum, imternal measurement 22sec ceeeeeeee 33.5 Dorso-ventral diameter of foramen mag- num, internal measurement ................-..--- 28.7 Height of occiput from plane of basioecipital Go) lamb dordail suture asec ane 2 areceece eee ecenee =e 79.6 Greatest width of muzzle at anterior end... 70 WG ferseanoy Che SNES) ee eee ee 114.5 Greatest width above orbits -..............-...-.---. 103.2 Least width behind orbits, in region of GOLOMANCS UU UT Cieccseese cece cece eeensoece eee 78.2 Width, measured across anterior ends of zygomatic processes of squamosals ........ 153.8 Least distance between outer sides of ptery- FEXOAUG OM EN IS per peers ae eee ere 61 Greatest height from ventral border of ptery- goid plate to highest elevation of frontals 134.7 a, approximate. MANDIBLE S.A. Rancho La Brea N. shastense No. 208 M. H. . 309 336.3 a135.4 46.2 23.6 43.2 38.2 shastense No. 313 M.H.S. A. Rancho La Brea N. 80.7 65.5 130.8 98.3 No. 632 M.H.S. A. Rancho La Brea N. shastense 313.6 24.2 78.5 73.9 111.9 104.3 78.5 No. 633 M.H.S. A. Rancho La Brea N. shastense 76.5 73.4 134.3 102.9 17 The crest of the occiput is N. shastense No. 634 M.H.S. A. Rancho La Brea The most striking characteristic of the lower jaw of Nothrothertum is its great similarity to that of Hapalops. regard is decidedly closer to the Miocene form than to its Pleistocene The former genus in this 1917] Stock: Skull and Dentition of Nothrotheriwm 149 contemporary, Megalonyxr. In general structure of: mandible Nothro- therium bears the same relation to Hapalops as Megalonyx does to Eucholoeops. The lower jaw of an apparently adult. individual, no! 208, of the Rancho La Brea species is approximately twice as large as that in Hapalops longiceps. Although the mandible may very closely approach Megalonyx in total length, yet it differs from that genus in its very decided slenderness. In both Hapalops and Nothrotherium the predentary portion of the jaw is produced anteriorly into a long beak which in the latter genus is also deeply concave. The edentulous beak or spout (fig. 5) is much more elongate than in Megalonyx. The anterior end may be rather acutely tapering as in no. 208 or rounding as in no. 456. —_—— Ke ae) A Fig. 5. Nothrotherium shastense Sinclair. Mandible, no. 166 M. H. 8S. superior view, X 1. Rancho La Brea Beds, California. — : As pointed out by Scott, the lower border of the ramus in Nothro- theriwm is less sinuous than in Hapalops. In the former genus it forms an even convexity which reaches its maximum development below the third inferior tooth. This border is more strongly convex than in Megalonyx, but decidedly less so than in Megathert ium. The inferior border posterior to the tooth series and reaching to the end of thé angular process is less decidedly concave in N othrotherium than: in Hapalops. The symphyseal keel is long and sharp, but not as prominent as in Megalonyx. Usually but a single mental foramen is present. In no. 456, however, a small opening is situated slightly above and posterior to the mental foramen of the right side. The horizontal limb of the ramus (fig. 6) is noticeably of less height, especially in the anterior region, and less robust than in Megalonyx. With the ‘disappearance 150 University of California Publications in Geology [ Von. 10 of the first tooth in Nothrotherium the deeply concave, outer wall of mandible between M; and Ms, occurring in Hapalops and Megalonyz, becomes greatly reduced and may be entirely absent as in no 166. There are frequently two foramina representing the postero-external opening of the dental canal in the Rancho La Brea species. In no. 208 two foramina are present on the left ramus and one on the right, an occurrence similar to that in a skull of Hapalops longiceps, no. 15523 Prin. Univ. Coll., while in no. 456 from Rancho La Brea there are two foramina on each side. The anterior foramen is situated on the outer surface of the ramus opposite the last inferior tooth and the second opening is at or shightly above the base of the ascending process. The coronoid process arises well to the outer side of Mz as in Hapalops, but it is relatively smaller than in the latter. It may be ds } Fig. 6. Nothrotherium shastense Sinclair. Mandible no. 166 M. H. S. A lateral view, X ¥%. Rancho La Brea Beds, California. broad as in no. 456 or rather narrow. The sigmoid notch, due to the high position of the condyle above the tooth row in Nothrotheriwm, is relatively much smaller than in the Miocene genus. In no. 208 the condyle in dorsal view has much the shape seen in Hapalops longiceps. In no. 456 and no. 418 the condyle has a greater oblique diameter and is more slender than in no. 208. The ventral notch between condyle and angle is relatively wider than in Hapalops, while the angular process in some specimens from the asphalt extends posteriorly as a more slender hook than in H. longiceps. The angle of the Jaw is much more slender in Nothrotherium than in Megalonyx. In M. jeffersoni the coronoid and angle are more nearly equally spaced on either side of the condyle than in the Rancho La Brea genus. The inferior border of the angle is deflected inward, forming a more pronounced shelf than in Megalony-. 1917 | Stock: Shull and Dentition of Nothrotherium 15 il < < 4 < 4 < . mH + “hy . . fe ssfaa] mas [--) mm mA anf sefan MEASUREMENTS OF MANDIBLE* Ones Ce Rey SA Se Say aAaQ aA SAQ seg 844 aA ee oars cote Se oe ZO. 408 gn 868 3ne 2 03.5 ano any avo gto «oy woe ZAC ZAM -CZaAe wae wee Zara Length from anterior end of sym- physis to posterior end of condyle 275mm. 277.1 a260.7 284.4 a267 Ses ee Distance from anterior end of sym- physis to anterior border of alveolus for M3 ............2.0.-022-2-------- 100.9 106.2 a96.8 104.7 100.38 20. ..... Distance from posterior border of alveolus for M; to posterior end (ity Bad ey eee eererers reer eee 121.2 134.6 a120 alee akon salaly(ea een eres Greatest length of symphysis .......... 90.4 903 SCS 270s 0.0: ZO an Wb eceecscoun Weceenece Greatest depth between M; and Mz, measured normal to tooth-row.... 56.6 60.6 54.2 56.1 53 61.3 61.6 Least height posterior to Mj............ 43 47.5 42 44.8 38.6 46.8 47.5 Greatest height from angle to coro- MLOVC PROCCSS .oeceeececee ces cacsaeeeezecceeszee 106.6 1214 uu. CALs yich AMON) ae eee Height of condyle above ventral order of angular process .......... AS eae es eee 26. 26.8 bord ft angular {| 9 26.4 26.8 Thickness of horizontal ramus at Mg 27.2 29.3 DOM ee 28:28 2 Dio eee cee seco Distance between inner alveolar borders of fourth cheek-teeth —.. 33 OU ile a eeereees Oe a eee eee ere * Where association of mandible with cranium is in doubt, the former is listed under a separate number. + This mandible may belong to cranium 313. a, approximate. DENTITION The dental formula in the Rancho La Brea Nothrotherium as in nate ‘ ey ees the Brazilian species is 33. In possessing a reduced dentition, Nothrotherium differs markedly from the certainly known Miocene Megalonychidae and Planopsidae as well as from the Pleistocene genera, Megalonyx and Megatherium. All the teeth are considerably smaller than in Megalonyx. The external layer of cement on the teeth may be only as thick relatively as in Hapalops. Supertor Series.—The tooth-rows extend very nearly parallel, the palate increasing slightly in width between the fifth cheek-teeth. teeth are more closely spaced than in Miocene genera. In the Rancho The La Brea species the largest interspace occurs between the alveoli of M4 and M®. Reinhardt states that in the Brazilian species of Nothro- therium the teeth are equally spaced. As in the various species of Santa Cruz ground-sloths the differ- entiation of the superior molariform teeth into a small M2, much 152 University of California Publications in Geology [ Von. 10 larger M2 and M4, and a M® greatly compressed anteroposteriorly, oceurs also in Nothrotherium although the distinction between M2 and M2 or M4 is not as marked in the former as in the latter. The teeth in Nothrotherium are noticeably more complex. This is indi- cated by the presence of distinct, median vertical grooves on the outer faces of M2, M2 and M4, and to a less extent also on the inner faces. Even M®, which is much more compressed anteroposteriorly than the other superior teeth, shows a distinct groove on the outer face and a much more faintly developed one on the inner. Nothro- therium, therefore, differs from Megalonyx in which such distinct lateral grooves are lacking on these teeth. In Hapalops indifferens the vertical grooving on the outer face of M2, M2 and M4 has been noted by Scott in some specimens. In describing the corresponding teeth, as Fig. 7. Nothrotherium shastense Sinclair. Right, superior, dental series no. 208 M. H. 8. A., occlusal view, natural size. First tooth to the right is M?. Rancho La Brea Beds, California. well as M®, in Hf. elongatus, Scott** states that ‘‘the vertical groov- ing of these teeth appears to be very capriciously present or absent.’’ Judging from the appearance of the occlusal surface, the outer com- pact layer of dentine in all the superior teeth of Nothrotherium is best developed on the anterior and posterior surfaces and_ least developed on the outer and inner sides. In M2, M2 and M4 this layer is shghtly thicker on the outer than on the inner surface. In M2 the layer is thickest on the posterior face, while on the outer and inner faces it is of equal thickness. M2 is smaller than M2 and M#. Contrasted with the latter teeth, M2 is relatively narrower transversely in Nothrotherium than in most species of Hapalops. It is relatively longer anteroposteriorly than in the latter genus. The tooth may be trapezoidal in shape, with anterior and posterior faces parallel as in no. 313, or these faces may converge to the outer side as in skull 208 (fig. 7). The anterior and posterior faces are nearly flat and the angles are well rounded. M2? thus differs from 28 Scott, W. B., op. cit., p. 218, 1903. 1917 | Stock: Skull and Dentition of Nothrotheriwm 153 the corresponding tooth in Megalonyx, which Leidy*® has deseribed as follows: ‘‘The second upper molar in section (Pl. XVI, Fig. 9, d), is quadrate with rounded angles. Its inner and posterior sides are the greater, and are nearly equal; and the remaining sides are also nearly equal, and are planes. The inner side is slightly convex, and the posterior side is nearly a plane and is directed obliquely outward.”’ On the occlusal surface the transverse valley between the anterior and posterior crests opens most broadly on the inner side in no. 208. In no. 313, on the other hand, where the transverse crests are parallel, the valley is of nearly the same width throughout. M2 and M4 are very similar in general shape. M# may be shghtly larger than M4, but the corresponding measurements of these teeth are usually very close. In the greater number of species of Hapalops, M2 is the largest of the molariform series, and this is true in general for the Santa Cruz Megalonychidae. In both teeth the anterior face is broadly convex and the posterior face concave. The anterior face rounds gradually to the external side; in other words, does not form a distinct angle with the outer side as in other cheek-teeth. The teeth do not narrow as much externally as in Megalonyx jeffersoni, in which respect they are more like J/. leidyi. They lack the typical quadrate cross-section characteristic of the corresponding teeth of Megatheriwm. In M2 and M4 the anterior crest of the occlusal surface is decidedly beveled in front, and the cutting edge of this chiseled surface is usually worn into a crescent. The transverse valley is worn most broadly on the inner side. In both teeth the postero-internal angle of the occlusal surface is subjected to greatest wear. In several loose teeth of Nothro- therium from the asphalt beds, referable to M2? or M4, the outer face is seen to be noticeably coneave in its longitudinal extent. This char- acter apparently distinguishes these teeth from M,; and especially from M5. M® resembles in its anteroposterior compression the corresponding tooth in Hapalops and in Megalonyx. It is approximately only one- half as long in that direction as the remaining superior cheek-teeth of Nothrotheriwm. The posterior face of M* in the species from the asphalt beds is very broadly coneave and the concavity may become quite deep as in a young individual, no. 640. The nearly flat anterior face, which is of less width than the posterior face, may have a median strip defined by a slight groove on each side. The inner face may have a faint vertical groove near the anterior border, while the outer face is 29 Leidy, J., op. cit., p. 17. 154 Unversity of California Publications in Geology [ Vor. 10 characterized by a well-marked median groove. On the occlusal surface there is no distinet valley formed, but the anterior edge is worn much lower than the posterior. This tooth differs decidedly from M2 in Megalonyx jefferson, which Leidy*® describes as follows: ‘‘The last molar is a smaller tooth than the preceding pair, but has nearly the same form in a reversed position, the base of the triangular section (Pl. XVI, Fig. 9, a) being outward. Its posterior side is transverse and is shghtly concave; and the anterior side is convex and directed obliquely inward.”’ Inferior series —With the loss of the first tooth in Nothrotherium the superior surface of the ramus directly in front of Ms is triangular in shape. The tooth-rows are relatively as far separated as in Hapalops . longiceps. They are very nearly parallel or diverge slightly pos- teriorly. In the Pleistocene genus the characteristic features of the three posterior teeth in Hapalops have been accentuated. Scott Fig. 8. Nothrotherium shastense Sinclair, Right, inferior, dental series no. 166 M. H. S. A., occlusal view, natural size. First tooth to the right is M3. Rancho La Brea Beds, California. oe describes these teeth in H. longiceps as follows: ‘**. .. 5 and gz are transverse and rectangular, and their raised margins are quite deeply notched on the inner and outer sides by the transverse valley; ; 1s subeylindrical, as in most of the other species.’’*! In M; and M, the denser, outer layer of dentine of the tooth crown is least developed along the outer and inner sides. It is perhaps less developed on the outer than on the inner side. The layer is thicker on the anterior and posterior faces of the crown, and appears slightly better developed on the posterior face. The thickness of this more compact layer of dentine determines in part the structure of the occlusal surface. The outer and inner walls which are thinnest, resist wear less, and are worn down more rapidly than the anterior and posterior walls. The latter are therefore prominent on the wearing * 30 Leidy, J., op. cit., p. 18. 31 Seott, W. B., op. cit., p. 182, 1903. 1917 | Stock: Skull and Dentition of Nothrotherium 155 surface as two transverse ridges with intervening valley excavated in the softer inner material of the crown. The type of wearing surface thus obtained resembles very much that in the larger teeth of MJega- therium, but in that genus the outer compact dentine is thinner and the cement (on the anterior and posterior faces) relatively much thicker. In the Rancho La Brea Nothrotherium the cement is more evenly distributed on the crowns of the teeth, with a moderate increase on the anterior and posterior faces in some specimens. In Megatherium there is an excessive thickening of the cement on the anterior and posterior faces. The complete length of the crowns cof Ms, My; and Mj is exposed in the somewhat broken specimen, no. 418. The teeth are seen to reach the inferior wall of the ramus, which is very thin. In this ramus the inferior teeth diverge upward in their course from the base to the alveolar border. In longitudinal extent the crown of M5 is slightly coneave posteriorly ; M; is practically straight posteriorly but slightly coneave laterally; M; evidently sloped posteriorly. M, and especially M; exhibit then a different longitudinal curvature from that shown by the third and fourth superior teeth. In M,; (fig. 8) the transverse width of the anterior half is distinetly less than that of the posterior half. The transverse axis of the tooth is oblique to the long axis of the tooth-row. This tooth differs from the corresponding one in Hapalops and Megalony. in the presence of median vertical grooves on the inner and outer faces. The anterior face is broadly coneave while the posterior face is correspondingly convex. On the occlusal surface the anterior transverse ridge is nearly straight and may be beveled in front, while the posterior is crescentic and is beveled behind. M, is shghtly larger than M; and narrows more toward the inner side. It is transversely placed with reference to the long axis of the tooth-row. In occlusal view it resembles somewhat the third and fourth superior teeth, but is in reverse position. If the tooth is oriented so that the posterior margin of the occlusal surface corresponds to the anterior margin of the third or fourth superior tooth, the former ean be distinguished by rounding less gradually toward the narrow lateral side. In other words, the third inferior tooth has all four angles better defined than those in the third and fourth superior teeth. This serves also to distinguish M; from either M* or M4. The vertical grooves of the lateral faces appear, as a rule, to be more sharply defined than in Ms, while the anterior half of the tooth is not as distinctly smaller 156 University of California Publications in Geology [ Vou. 10 transversely as the posterior half. M; differs from the corresponding tooth of Hapalops and Megalonyx in the presence of well-marked lateral grooves. The anterior and posterior faces resemble those in M5. MEASUREMENTS OF DENTITION Greatest length of su- perior molar series, alveolar measurement M?, greatest anteropos- terior diameter M2, greatest transverse diameter M, greatest anteropos- terior diameter ........ M’, greatest transverse diameter M+, greatest anteropos- terior diameter M+, greatest transverse diameter M$, greatest anteropos- terior diameter MS, greatest transverse diameter Greatest length of in- ferior molar series, alveolar measurement Ms, greatest anteropos- terior diameter ........ Ms, greatest transverse diameter Mz, greatest anteropos- terior diameter Mz, greatest transverse diameter M;, greatest anteropos- terior diameter ........ M;, greatest transverse diameter * This specimen may a, approximate. 2 ce ee ae ig ae Soe ee eee ref] ssf) ma im tm tm aud 3 Bu 3 me mefe eg Bebe qa g2Q 8=9 839 8eg gaa “Se 4Sg Bhs 4Bs 4Bs Bag one ee Se ene we is ~0O8 OS ~O8 ~oOs ~O8 ~O8 aze 2ae wae 2am Azam wze 61.6 mm, 62.8 61.5 DUD 62.3 65.4 12 12 Taal 3)sereeeee 12.4 12.9 1183 3 COLOR teens 14.3 ee 1133-33 118) al4 ae 13.8 Bankes 16.8 16.9 a@l6.8 ........ 18.9 Mee 1133 12.8 Wey sees 12.1 IL7f Mie Ils iil eseres 18.3 Sui 7.6 (eB aids? 8.8 ig96 144 198 @f29 can. 16 No.636* No.456 No.418 No.637 No.638 Dil 54.7 ON 59 51.7 49.4 3 G ee ee 13.6 13.9 al12.5 TGS aera eee 17.6 15.9 al16.3 14.2 al 3) eee ee 14.1 al4.7 11533 NYE WED es 18.4 16 16.4 14 5} 14 apy Oe ee 14.5 15.6 15:8 15 G22 eens 15 , belong to cranium 313. No. 639 M.H.S. A. Rancho La Brea N. shastense 11.5 48.5 all.8 al6.2 13.4 16.4 < < ns ae 7H SH gue gh gaa gF4 hoo Gro ata ats toe hoe -O8 ~O8 2246 ware 9.7 9.9 11.2 11.9 1) ee 14.4 wu... Ich esas IB HSY Slates 7.2 7.5 10.5 11.3 The single tooth, no. 10495 Univ. Calif. Coll. Palae., of Nothro- theritum previously described by the writer from Rancho La Brea, was assigned to the superior dentition chiefly on similarity of its cross- section to that of the second alveolus. It was remarked, however, that the Rancho La Brea specimen differed from no. 8702 from Potter 1917] Stock: Skull and Dentition of Nothrotherium 157 Creek Cave in longitudinal curvature. The longitudinally concave, posterior face of no. 10495 and the distinctness of the angles of the occlusal surface relate this specimen much more closely with the second inferior tooth than with either the third or fourth superior teeth. The occlusal surface resembles also that of Mz. No. 10495 is then either a second or third inferior tooth. The last inferior tooth, which in Hapalops is more or less eylin- drical in shape, retains the rounded internal side in Nothrotherium. It thus agrees with Megalonyx in differing markedly in shape from either M; or My. This tooth in Megatherium, although smaller and relatively longer anteroposteriorly than M; and Msg, is essentially of the same shape as the other inferior teeth. The transverse axis of M; in Nothrotherium is directed obliquely to the long axis of the tooth-row, thus resembling Hapalops and Megalonyxr. On the outer flattened face of this tooth a median vertical groove may be slightly defined as in no. 208, or well defined as in no. 456. In the presence of this groove, Nothrotherium differs from Hapalops and Megalonyx. The outer anterior and posterior corners of Mj; are well rounded. The denser layer of dentine is best developed on the inner and posterior sides and least on the outer side. The border of the occlusal surface is least worn at the middle of the inner side and at the postero- external corner. Between the resulting prominences, the border is beveled posteriorly. In Megalonyx the occlusal surface of the corre- sponding tooth is somewhat similarly worn. It is described by Leidy ce as having . a transverse valley, whose boundaries are most prominent at the antero-internal and postero-external angles.’’*? REVIEW OF SPECIES In a former note** the writer briefly described a single skull of Nothrotheriwm without mandible from Rancho La Brea, which was referred to a new species, V. graciliceps. At that time the only other material of this genus available from the asphalt was a single tooth, no. 10435, in the palaeontological collections of the University of California. In a comparison of the Rancho La Brea Nothrotheriwm with N. shastense from Potter Creek Cave, it was inferred that the lower jaw in the former species was longer than in the latter. The principal difference, however, between the two forms was thought to rest in the shape of the last superior tooth. 82 Leidy, J., op. cit., p. 19. 33 Univ. Calif. Publ. Bull. Dept. Geol., vol. 7, pp. 341-358, 1913, 158 University of California Publications in Geology — (VoL. 10 In addition to the skull material contained in the collections of the Museum of History, Science and Art of Los Angeles, there are also available for comparison five mandibles as well as fragments of mandibles of Nothrotherium from the asphalt beds. These specimens show a considerable range in size. No. 636 represents one of the smaller individuals and approximates very closely in size the frag- mentary ramus. no. 8422 Univ. Calif. Coll. Palae., from Potter Creek Cave. The latter if anything is slightly smaller than no. 636. The differences between the specimens are slight. The tooth-row in no. 8422 is a trifle longer; the postero-external opening of the dental canal is small and the ascending portion of the ramus behind M; is apparently a lttle thicker than in no. 636. On the whole the char- acters presented by the fragmentary ramus from Potter Creek Cave are hardly to be distinguished from those of the Rancho La Brea specimens. Associated with the ramus of V. shastense from Potter Creek Cave are a number of teeth, one of which Sineclair** identified as a last superior tooth. He describes this specimen as follows: ‘‘It is a tri- angular tooth with the posterior side plane, the anterior convex, and the outer plane and meeting the posterior at a right angle.’’®* A com- parison of this tooth with the last superior alveolus of skull 15 from Rancho La Brea showed that the latter must have possessed a M?* which differed markedly from Sinclair’s specimen. This has been amply verified by the additional material now available. The shape of the tooth in the species from the asphalt beds is remarkably con- stant. It differs from the corresponding tooth, no. 8497 Univ. Calif. Coll. Palae., from Potter Creek Cave in (1) subtrapezoidal outline, (2) outer and inner sides of equal thickness, (3) posterior face con- cave transversely, (4) presence of vertical groove on outer face and faint vertical groove on inner face near anterior border, and (5) outer and anterior faces coneave longitudinally. The differences noted are undoubtedly great enough to separate the Rancho La Brea form as a distinct species, if Sinclair’s specimen can be regarded with certainty as a last superior tooth of Nothro- therium. A eritiecal re-examination of this tooth has convinced the writer that there are, however, serious objections to its being considered as such. As stated by Sinclair, no. 8497 (fig. 9) has been somewhat "84 Sinclair, W. J., New mammalia from the quaternary caves of California, Univ. Calif. Publ. Bull. Dept. Geol., vol. 4, pl. 23, fig. 8, 1905. 35 Sinclair, W. J., ibid., p. 154. 1917] Stock: Skull and Dentition of Nothrotherium 159 injured by rodents, especially toward the occlusal surface. The onawed surfaces of the tooth do not seem to account entirely for the difference in size of the two ends: that is to say, the tooth narrows toward the occlusal face. This is considered as characteristic of immature individuals. It is apparent also that this tooth is excep- tionally large in comparison with the remaining teeth of Nothrotherium shastense. Furthermore, there are several teeth in the collections from Potter Creek Cave which are not clearly referable to Nothrotherium, but belong perhaps to a small species of Megalony.r. In faet, Sinclair deseribed a specimen, no. 8203, from the cave deposit which he identified tentatively as belonging to Megalonyx wheatleyi. With the fifth superior tooth of MW. jeffersoni no. 8497 from Potter Creek Cave agrees in triangular shape but differs in size. The latter specimen Fig. 9. Megalonyx(?), sp. M5, no. 8497, Univ. Calif. Coll. Palae., anterior view with outline of section through pulp-cavity, natural size. Potter Creek Cave, Shasta County, California. lacks possibly ‘‘the slightly concave’’ posterior face noted by Leidy in M. jeffersoni, but this can only be regarded as a minor difference. In a former note the writer considered specimen 8337 from Potter Creek Cave as probably representing an inferior tooth. The characters seen in occlusal view relate this specimen much more closely with Ms; and M; than with M* or M4. The concave posterior face in its longi- tudinal extent is a character held in common by no. 8337 and Ms; of Nothrotheritum from Rancho La Brea. The tooth from Potter Creek Cave differs sightly from the second and third inferior teeth from the asphalt beds in having the four angles of the occlusal surface shghtly more sharply defined. While the comparatively large size of no. 8497 is in itself not sufficient reason for generic determination as other than Nothro- thertum, in view also of its much closer resemblance to the fifth superior tooth of Megalony« the identification with the latter is more probable than with Nothrotheriwm shastense. The fragmentary 160 University of California Publications in Geology — | Vou. 10 ramus, no. 8422, from Potter Creek Cave, presents but insignificant differences when contrasted with specimens from Rancho La Brea. In addition to no. 8497, a number of upper and lower teeth were regarded by Sinclair as pertaining to N. shastense. These specimens resemble closely in size and shape corresponding teeth of the Rancho La Brea species. Unless other characters favoring a specific separation of the Rancho La Brea material are revealed, NV. graciliceps must be regarded therefore as synonymous with N. shastense. Dr. O. P. Hay*® has recently described as a new species, Nothro- therium texanum, a damaged skull possessing the superior dental series of one side but lacking the lower jaw. The specimen is reported to have come from northern Texas, presumably from Pleistocene deposits. As indicated by Dr. Hay comparison between the Texas species and N. shastense from Potter Creek Cave is restricted to loose teeth found with the type ramus of the latter species. Of these, he considers speci- mens figured by Sinclair®’ as representing the second and third teeth. Specimen 8702 from Potter Creek Cave, represented in figures 3 and 3a of Sinclair’s paper agrees very closely in size with the second superior tooth of N. teranum. Dr. Hay believes that the teeth of N. teranum ean be distinguished, for in no. 8702 ‘‘both the front and the rear faces are convex in section, whereas both the second and the third teeth of NV. teranum have the front face convex and the rear face coneave.’**S In no. 8702 from Potter Creek Cave the posterior face is not entirely convex, for as is shown in section there is developed toward the outer side a slight but nevertheless distinct concavity. Furthermore, in teeth from Potter Creek Cave, representing either M2 or M4 of the superior dental series, the depth of this concavity may vary greatly. Tooth 8337 from Potter Creek Cave, represented in figures 5 and 5a of Sinclair’s paper, is regarded by Hay as being the third (M+) of the superior series. In the previous note on the Rancho La Brea Nothrotherium the writer stated that no. 8337 is probably of the inferior dentition, a view which is still maintained.*® 36 Hay, O. P., Descriptions of two extinct mammals of the Order Xenarthra from the Pleistocene of Texas, Proc. U. 8. Nat. Mus., vol. 51, pp. 107-123, pls. 3-7, 1916. 37 Sinclair, W. J., New mammalia from the quaternary caves of California, Univ. Calif. Publ. Bull. Dept. Geol., vol. 4, pl. 23, figs. 3, 3a, and 5, 5a, 1905. 38 Hay, O. P., ibid., p. 121, 1916. In the present paper the superior teeth of Nothrotherium regarded by Hay as second and third have been designated M® and Mé respectively. 39 Vide supra, p. 159. 1917 | Stock: Skull and Dentition of Nothrotherium 161 The fifth superior tooth, no. 8497, from Potter Creek Cave, re- ferred to Nothrotherium by Sinclair, has been shown above to resemble Megalonyx much more closely. It undoubtedly does not pertain to the former genus. The characteristic features exhibited by this speci- men cannot then be used as distinguishing Nothrotherium shastense. It is evident from the above discussion that it is not possible to separate N. texanum from N. shastense on the basis of characters at present available. Dr. Hay considers the Texas form as very closely related to the Rancho La Brea species of Nothrotherium, as indicated by a com- parison with skull 15 contained in the collections of the Museum of History, Science and Art of Los Angeles and described by the writer in 1913. He remarks, however, that ‘‘One can not rely wholly on the differences which are seen in the two skulls for additional specimens 2740 may be intermediate. The characters exhibited by the teeth of N. teranum fall easily within the range of variation of teeth in Rancho La Brea skulls. One of the important skull characters cited by Hay as distinctive of N. teranwm is the structure of the pterygoid bulla. In the Texas specimen the bulla of each side is open wide below, in which respect it is in marked contrast to that of Rancho La Brea skulls. In the latter the pterygoid bullae when undamaged are always com- pletely closed below with the exception of an elongate orifice on the inner ventral side. The pterygoid bulla in the skull of Nothrotheriwm from Brazil, described by Reinhardt, lacks even this internal opening and is apparently complete. Judging from the damaged condition of the skull of N. teraniwm (the palate being severely injured and the pterygoid plates entirely broken away in that specimen), such fragile structures as the ptery- goid bullae ean hardly be expected to remain entire. It is then reason- able to suppose that the present appearance of these bullae in the Texas specimen is to be attributed to injury sustained during preservation. Dr. Hay is, however, of the opinion that the pterygoid bulla in NV. feranum remained widely open below during the life of the indi- vidual. He states: ‘‘The bulla of NV. feranum appears not to have had a floor. The pterygoids seem to form a wall whieh surrounds the cavity on both sides. On the median side the edge of the wall is partly intact, partly injured. On the outer side the wall comes down to a sharp thin edge which appears to be little if at all injured. In places the edge is certainly wholly natural. Such being the case 40 Hay, O. P., ibid., p. 121, 1916. 162 University of California Publications in Geology [ Vou. 10 the bulla is incomplete and is a cavity opening below by a mouth 30 mm. wide.’ Of other skull characters considered by Hay as distinetive of N. feranum mention may be made of the dorso-ventral diameter or height of muzzle and combined width of the nasals. In contrast to no. 15 additional skulls now contained in the collections of the Museum of History, Science and Art of Los Angeles approach the Texas specimen much more closely in height of muzzle. This is particularly true of no. 166 in which the height is 49.2 mm. The combined width of the nasals in the latter skull corresponds almost exactly with that in N. teranum. RELATIONSHIPS OF GENUS In this paper it is proposed only to touch upon some of the most significant relationships of Nothrotherium as brought out in a study of the skull and dentition. The skeletal elements, associated with the skull material in the Museum of History, Science and Art of Los Angeles, furnish also a wealth of evidence concerning relation to Miocene and Pleistocene ground-sloths, and until the whole skeleton can be fully studied it is perhaps premature to enter on a final con- sideration of the systematic position of the genus. The many resemblances between Nothrotherium and Hapalops, as shown by the foregoing comparisons, strongly support the view that the former genus is derived from Hapalops as held by Scott. More recently F. Ameghino**? in a discussion of the Miocene relatives of Nothrotheriwm derives the genus from a Hapalops-like form. It is not clear which genus he considers closest in this Miocene ancestral relationship,** for in one phyletie scheme he derives Nothrotherium from Trematherium while in another he considers the genus as descend- ing from Yyophorus. According to Scott, Trematheritum is very imperfectly known, while Yyophorus 1s synonymous with Hapalops. As already noted, the type of skull characteristic of Nothrotherium has deviated less from the more generalized type of the Miocene Megalonychidae than has Megalonyx. The differences between Nothrothertum and Megalonyxs, which in many respects make them 41 Hay, O. P., tbid., p. 119, 1916. 42 Ameghino, F., Notas sobre una pequefa coleccion de huesos de mamiferos procedentes de las grutas calecaAreas de Iporanga en el Estado de Sao Paulo- Brazil, Revista do Museu Paulista, vol. 7, pp. 99-119, 1907. 48 Ameghino, F., ibid., pp. 105 and 119. 1917 | Stock: Skull and Dentition of Nothrotherium 163 very dissimilar in structure of skull, are to be considered as end- products of two widely divergent lines of evolution arising from more closely related forms in the Tertiary. The writer is thus entirely in accord with Scott, who states with reference to the Santa Cruz ground- sloths: ‘‘ That Hapalops is nearly related to both Nothrotherium and Megalonyx is abundantly clear from a cursory examination of the skeleton, all parts of which are very similar to those of the two Pleistocene genera. In fact, there is every reason to believe that Nothrotherium was the direct descendant of some species of this genus.’ 44 With a reduced dentition, Nothrothertum is not only more special- ized than Hapalops, but is also more advanced than either Megalony.c or Megatherium. In a comparison of the two Pleistocene megalonychids, oe Ameghino states: ** Pero en cambio, Megulony.c que tiene cinco dientes en cada lado aparece como una forma considerablemente mas primitiva que Nothrotherium que solo tiene cuatro.’ Judging from the struc- ture of the skull, the position of the molariform teeth in Nothrotherim undoubtedly corresponds to that of the four posterior teeth of Megalonyr. Thus a closer relationship between these genera than between Nothrotherium and Megatherium is indicated by the position of the molariform teeth. This resemblance extends also to the shape of these teeth. In Nothrotherium and Megalonyx M2 is smaller than M® or M4 and this is usually true also for Hapalops; M* as a rule can be distinguished from M# by its slightly larger size; M® is compressed anteroposteriorly. In the inferior molariform series the principal character held in common (with shght modifications) by the three genera is the shape and position of M;. In Hapalops this tooth is sub-cylindrical, while in Nothrotherium and Megalonyx it has essentially the same shape but with the outer side fattened. Further, in the three genera the trans. verse axis of M; is somewhat oblique to the long axis of the tooth-row. In Megatherium this tooth is quadrate in shape, and transverse in position, thus resembling the remaining inferior teeth. CONCLUSIONS Next to Mylodon, the genus Nothrotherium is the most abundant ground-sloth found at Rancho La Brea. It is represented by decidedly fewer individuals than is Mylodon. The occurrence of Nothrotheritum 44 Scott, W. B., op cit., p. 181, 1903. 15 Ameghino, F., op. cit.,-p. 103. 164 University of California Publications in Geology [ Vou. 10 in the asphalt beds in greater numbers than Megalonyxz is singular, considering the apparently more restricted range of the former genus in North America. There is reason for believing, however, that Nothrotherium flourished in California and Texas during a portion of the Pleistocene. The species of Nothrotherium from the asphalt beds, originally considered by the writer as new, is now held to be identical with N. shastense Sinclair from Potter Creek Cave. Further investigation may justify a subspecifie separation of the Rancho La Brea form, but at present there is not sufficient reason for a specific distinction from the Potter Creek Cave species. The many characters held in common by WN. teranwm and N. shastense from Potter Creek Cave and Rancho La Brea suggest specific identity of the two forms. Nothrotherium is very closely related to the Miocene genus Hapalops. Comparison between the two genera presents nothing which can be considered adverse to the view held by Scott, that Nothrotherium is the direct descendant from Hapalops. The Pleisto- cene genus shows several noticeable advances beyond the Miocene form in skull and dentition. The structure of the skull in Nothro- therium indicates a type which has deviated less than Megalonyx from a generalized skull characteristic of the Santa Cruz ground-sloths. The great dissimilarity between Nothrotherium and Megalonyx in many characters of skull and dentition substantiates the views of Scott and Ameghino that these genera are the results of two divergent lnes of evolution already separate in the Santa Cruz Miocene. The differ- ences between the two Pleistocene genera are in many instances so great as to suggest a separation of subfamilies rather than genera. 171 (Cy rat SUSI GaN Sg 174 INTRODUCTION Opportunity has recently been afforded the writer to examine the very extensive series of mylodont skulls from Rancho La Brea contained in the collections of the Museum of History, Science and Art of Los Angeles. This series consists of thirty-two erania and a number of mandibles, for the most part well preserved, together with other skull material not in as favorable a state of preservation. The splendid collection at the Museum in Los Angeles rivals in wealth of material the great collections of Pampean ground-sloths in South American museums. In examination of the Los Angeles series of skulls a number of interesting points presented themselves which were not touched upon, or were but little discussed, in the preliminary report by the writer? on the University of California series. Several of the skulls examined were found to differ in certain features from the broad type character- 1 Stock, C., Skull and dentition of the mylodont sloths of Rancho La Brea, Univ. Calif. Publ., Bull. Dept. Geol., vol. 8, pp. 319-334, 1914. 166 University of California Publications in Geology [Vou. 10 istic of Mylodon harlani from Rancho La Brea, and as these characters are apparently constant and cannot be satisfactorily shown to grade into the usual type of skull from the asphalt deposits, they are con- sidered to represent a new subspecies. It may be possible to establish a series with uniform and perfect gradations between the narrow and broad types of skulls of M. harlani when the entire mylodont sloth collection is reviewed, but at present it seems necessary to make the distinction between the two forms. I desire to acknowledge my thanks to Mr. Frank 8. Daggett, Direc- tor of the Museum of History, Science and Art of Los Angeles, who not only very kindly allowed me to examine the ground-sloth material but rendered many personal favors during my stay at the Museum. I desire also to thank the other members of the staff for many cour- tesies shown me. The photographs of the skull of the new subspecies were taken at the Museum by Mr. L. E. Wyman. CRANIUM Of the thirty-two skulls of mylodont sloths contained in the Rancho La Brea collections of the Los Angeles Museum of History, Science and Art, by far the greater number range approximately between 460 mm. and 525 mm. in length (from anterior end of maxillary to posterior end of occipital condyles). None of the skulls attain the length of the Colorado specimen deseribed by Professor Cockerell.? With the exception of three, possibly four crania, this series is com- posed of skulls having the general characteristics already discussed in connection with a similar series contained in the palaeontological collections of the University of California. Specimens 642, 643, 646, and 695 * differ from the usual broad type of skull of Mylodon harlani from Rancho La Brea in the decidedly more slender cranium posterior to the postorbital processes. For skull 642 this is distinctly indicated in plate 3. In this respect they ap- proach more closely the skull-form in Mylodon garman, differing, however, in being much less slender. With the least width of the skull behind the postorbital processes as a convenient and suitable index of slenderness of the cranial case, a series can be established with gradations tending toward the broader type of skull. The speci- 2 Cockerell, T. D. A., A fossil ground-sloth in Colorado, Univ. Colo. Studies, vol. 6, pp. 309-312, 2 pls., 1909. 3 All numbers used in this paper, unless otherwise stated, are the catalogue numbers of specimens contained in the Rancho La Brea collections of the Museum of History, Science and Art of Los Angeles. 1917] Stock: Skull Structure of Mylodont Sloths 167 men showing the greatest constriction is no. 646, while nos. 642, 643, and 695 show successively less constriction. The Nebraska skull de- scribed by Barnum Brown? is slightly more constricted than no. 646, but the actual difference is so small that it is negligible. In this arrangement, the skulls, including the Nebraska specimen, exhibit a variation in length of approximately only 30 mm. In a former paper the writer’ stated that the inflation of the muzzle in the mylodont skulls of the University of California series was similar to that in the Nebraska skull. This is true also for the greater number of skulls contained in the Museum of History, Science and Art of Los Angeles, as far as the actual diameter of muzzle is eoneerned. In proportion to the postorbital constriction, however, many of the skulls, including the slender types, are slightly less inflated at the muzzle than Brown’s specimen. The palate posterior to the fifth superior tooth is very narrow in the slender type of skull from Rancho La Brea. This character apparently does not depend on the slenderness of the cranium, since in M. garmani the palatal index is actually greater than in a broad skull of M. harlani (no. 21158 Univ. Calif. Coll. Palae.) of approx- imately the same length. Furthermore, in no. 21160 Univ. Calif. Coll. Palae., a narrow palate, which is 57.5 mm. in width, is associated with a broad cranium. The slender skulls again lend themselves to a gradational arrangement, which, however, is not the same as for the cranial index. No. 642 possesses the least width of palate posterior to the fifth tooth, the transverse diameter gradually increasing in skulls 646 and 643. The Nebraska skull in this character follows no. 648. In none of the skulls contained in the Museum of History, Science and Art is the fifth superior tooth as little removed from the middle of the postpalatine notch as in Brown’s specimen, or as far removed as in the skull deseribed by Cockerell. The flattened dorsal surface of the brain-case, outlined by the occipital crests, varies in width irrespective of the degree of slender- ness of the cranium. In the slender skulls the width of this sur- face may be equal to or greater than in some of the broader types. In skull 707 the dorsal surface of the cranium is very wide, thus differ- ing from the remaining skulls from the asphalt beds and resembling closely Mylodon robustus as figured by Owen.® 4 Brown, B., Bull. Amer. Mus. Nat. Hist., vol. 19, pp. 569-583, pls. 50-51, 1903. 5 Science, n.s., vol. 39, pp. 761-763, 1914. 6 Owen, R., Description of the skeleton of an extinct gigantic sloth, ete. (London, 1842), pl. 3. 168 University of California Publications in Geology (Vou. 10 MANDIBLE A number of mandibles together with separate rami, some of which are directly associated with crania, are also in the collections of the Museum of History, Science and Art. These exhibit the degree of variation already discussed in connection with the University of California series of lower jaws. In general the ramus decreases noticeably in height from the base of the coronoid process to the anterior side of the first lower tooth. Occasionally, as in no. 696, the height of the ramus in front of the first tooth is much greater, and resembles M. garmani and M. robustus as well as no. 21576 Univ. Calif. Coll. Palae. In no. 696, also, the inferior dental canal of the right ramus opens anteriorly by three foramina. The latter variation from the normal number of two occurs quite frequently, much more so than the occurrence of only a single open- ing. The greatest predental width of the mandible is always less than the distance between the first tooth of each side. Unfortunately there are no mandibles directly associated with the three exceptionally slender skulls. An incomplete and badly worn mandible, showing the complete lower dentition on one side is, how- ever, associated with no. 695. This specimen exhibits a remarkable abnormality in the presence, anterior to the first inferior tooth, of a distinct alveolus for an extra tooth. It is present only on the right ramus, where it is 9 mm. in advance of the normally placed first tooth. The alveolus measures 11 mm. in anteroposterior diameter by approx- imately 9 mm. transversely. DENTITION The thirty-two skulls contained in the Museum of History, Science and Art of Los Angeles exhibit a variation in the superior dentition similar to that noted in the University of California series, namely : 1. Skulls with four teeth on each side of the palate. 2. Skulls with four teeth on one side of the palate and five teeth on the opposite side. 3. Skulls with five teeth on each side of the palate. The three, possibly four, slender skulls show the following vari- ation: nos. 646 and 643 possess the normal number of five functional teeth on each side of the palate, no. 695 is an example of the second group, in which there are five teeth on one side and only four on the opposite side of the palate, and no. 642 had only four functional teeth on each side of the palate. 1917] Stock: Skull Structure of Mylodont Sloths 169 This splendid series of specimens receives added importance in that it demonstrates completely how the first tooth of the superior series may disappear. In skull 694, a specimen originally of the third eroup, the alveolus for the first tooth is very well developed. On the left side of the palate the first alveolus was originally as well developed as on the right side. Around the border of the former alveolus an irregular, spongy growth of bone is formed which shows a tendency to grow toward the middle of the tooth-socket. That this actually takes place is well exhibited by no. 642, in which the closure of the first superior alveoli has progressed much further. In this skull the first alveolus of the left side is almost completely closed, while that on the right side has a shallow, crescentic opening along its lingual border. No. 693 illustrates how the entire alveolus may be filled by a spongy growth of bone. The final stage is reached in no. 21156, Univ. Calif. Coll. Palae., for example, or in the Nebraska skull described by Brown, where the first superior tooth has entirely disappeared, its former presence being indicated by a sear in front of the second superior tooth. It is interesting to note in this connection that somewhat similar observations on the closure of the first superior alveoli in South American mylodonts have been made by Burmeister,‘ who states: . . . . Der Schadel des hiesigen Museums [a skull referred to Grypotherium and contained in the collections of the Museo Nacional at Buenos Aires] hat noch offene Alveolen im Oberkiefer; in dem von Reinhardt abgebildeten Schidel sind sie schon ganz mit Knochenmasse gefiillt, aber als Narben sichtbar geblieben. Whatever the initial cause of the disappearance of the first superior tooth may have been, it is certain that in some cases the tooth was well developed at the time of its disappearance. It is conceivable that the tooth may have broken off during the life of the individual, an accident which might readily have oceurred, consider- ing the habits of the animal. A rapid growth of bone around the periphery of the alveolus may perhaps have prevented the tooth again becoming functional, and as a result resorption took place. It does not seem probable that such resorption was due to old age alone, although this may also have been a factor. In other skulls variation in size of the first tooth favors the idea that growth may in some indi- viduals have been inhibited from the start. In no. 21158 Univ. Calif. 7 Burmeister, H., 8.-B. Akad. Berlin, p. 1132, 1886. 170 University of California Publications in Geology [Vou. 10 Coll. Palae., for example, the first tooth, present only on the right side, was very diminutive. It is therefore not improbable that in some skulls the development of the first tooth may have been completely arrested. As already stated, there are no mandibles directly associated with nos. 642, 643, and 646. ) (Se) a, approximate. 174 University of California Publications in Geology (Vou. 10 MEASUREMENTS OF DENTITION < < ad < 2h s nig sug ws Qa. Qe RC ieaes ~H gia 0 Sed Gee He i des Eas pas “9g 0 "gg dg Ges see: ee aoe 4 ae Age a2e fae 228 M2, anteroposterior diameter ........................-- @I33.5mM, 4 eee a31.8 M?, transverse diameter ..............--.-----sc-ecceece-- Qut8.3 0 ee eee 20. M3, anteroposterior diameter .......................-- a28.6 a23.2 o... 28.3 Me rian S Verse (AMC tel seescee een eeeeeneeee ees a24.3 a20;3 eae 23. M, anteroposterior diameter .................-...-..---- 22. G20:4, «225 | ee IMG, transverse’ diameter 22.2... cee ee 23.8 Doc 0 ae ae M2, anteroposterior diameter ..................-2----- a27.3 2253) eeeeeee 5.6 M5, transverse diameter ........---....-----:--::-+---+- a20, USS.5 Wee 22.4 Length of superior series, from anterior end of first alveolus to posterior end of fifth BIV COMI: sscectcce-acseccresesrecezecacecee eiceeetaeeerestrseeears 146.5 QUST.) 0 ee eee Length of superior series, from anterior end of second aveolus to posterior end of fifth Eas £ 210) RES] s eee pisces See rene eeee Ue ne ABMEMES aan EE Le ree 119.6 TINKCORS} 9) 9 eps 120.6 IMG. amteroposterlor «(tame Cer csccesrecceseece neces == eee ereeuneeeo==ee a14.5 ..... Mir, mLBAMISVCTS@. aM CLC ese resstcseaccecesscteseen cava atias=ce- fm eeee===s Q@4 oa. Ms, anteroposterior diameter —-.--2 cece fees estes PASE ee te IMGs dmamsverse diameter c.se-seeseese ces ceee eee rere eee uzeuere 20:2) = Mz, diameter of occlusal surface normal to PaEh Neen ODEN A) Ry ee een nS cee I, | S228 Mz, anteroposterior diameter. 2.c.ccecce eee ete 525 9 eee M,, greatest diameter of anterior lobe... 9° eae UPS, eth Mj, greatest diameter of posterior lobe ........0 0 22-2 00000 wees QUO ts ee Length of inferior series, alveolar measure- 18.5) 0 ee ie Pee Se eee a 130:4 sae. a, approximate. al, alveolar measurement. CONCLUSIONS The following additional facts have been noted with reference to the mylodont skull series from Rancho La Brea: Three, possibly four, crania contained in the Museum of History, Science and Art of Los Angeles, are recognized as representing a form subspecifically distinet from typical Mylodon harlani. These crania differ from M. harlani of Rancho La Brea in exhibit- ing in combination a rather narrow brain-case with a narrow palate posterior to the fifth tooth. The Nebraska skull described by Brown can not be referred to the new subspecies from Rancho La Brea, since its characters, although in certain respects approaching those of the latter, are still quite distinct. The Nebraska specimen presumably represents Mylodon harlani, but may belong in a subspecies distinct from the two known to occur at Rancho La Brea. Transmitted December 23, 1916. ) ee . EXPLANATION OF PLATE 3 Mylodon harlani tenuiceps, n. subsp. Cranium, no. 642 M. H. 8. A., superior view, approximately three-eighths of natural size. Rancho La Brea Beds, Cali- fornia. Photograph by L. E. Wyman. [176] WINIVer CALIE: PUBE, BULL) DEPT: GEOL: fiSmOCK I VOE. l0;4PRE: EXPLANATION OF PLATE 4 Mylodon harlani tenuiceps, n. subsp. Cranium, no. 642 M. H. 8. A., inferior view, approximately three-eighths of natural size. Rancho La Brea Beds, Cali- fornia. Photograph by L. E. Wyman. [178] UNIV, CALIF. PUBL, BULL. DEPT. GEOL [STOCK] VOL. 10, PL: TEM. ION OF SEVERAL ERICAN TERTIARY LAGOMORPHS - BY LEE RAYMOND DICE — - _ UNIVERSITY OF CALIFORNIA PRESS ~ BERKELEY eations of learned societies and institutions, univ all the publications of the University will be sent upon reques publications and other information, address the Manager of ‘the U: California, U. S. A. All matter sent in exchange should be addressed to Department, University Library, Berkeley, Bee, U.S. A. Otto HARRASSOWITZ ‘aR. FRIEDLAENDER & So: LEIPZIG : ‘ BERLIN Agent for the series in American Arch- Agent for the series in Ame aeology and Ethnology, Classical Philology, aeology and Ethnology, Agricn aay C Economics, Education, History, Modern Botany, Geology, Mathematies, P: Philology, Philosophy, Psychology. Physiology, Zoology, and Memoirs. — Geology.—ANDREW C. Lawson and JoHN C. Merriam, Editors. Price, volumes 1-7, volumes 8 and following, $5.00. .--cs2eec2--c e.g" : het all the publications of the ate te will ba sent upon reques publications and other information, address the Manager of the Univ California, U. S. A. All matter sent in exchange should be addresse Department. University Library, Berkeley, California, U. S. A. - Orro HARRASSOWITZ a: LEIPZIG Hee Agent for the series in American Arek: ‘Agent for the series in J aeology and Ethnology, Classical Philology, aeology and Ethnology, Agricult: Economics, Education, History, Modern Botany, Geology, Mathematic Philology, Philosophy, Psychology. Physiology, Zoology, and Mem Geology.—ANDREW C. LAwson and JoHN C. MeERgIAM, Editors. Price, volumes 1- volumes 8 and following, $5.00. : Cited as Univ. Calif. Publ. Bull. Dept. Geol. Volume 1, 1893-1896, 435 pp., with 18 plates, price ...........-..ceccccssccencenseoeroee= Volume 2, 1896-1902, 457 pp., with 17-plates and 1 map, price ............-..- Volume 3, 1902-1904, 482 pp., with 51 plates, price .......c.-.-sssscecsce-se-0 Volume 4, 1905-1906, 478 pp., with 51 plates, price ......... : Lene fs Volume 5, 1906-1910, 458 pp., with 42 plates, price .......-.2-:::--:e0--!- A list of titles in volumes 1 to 5 will be sent upon request. VOLUME 6. 2 . The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller......... re . Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northweste Nevada, by John C. Merriam. Part I.—Geologie History.....v.-.------c-sccce-eneenes The Geology of the Sargent Oil Field, by William F. Jones ................. Additions to the Avifauna of the Pleistocene Deposits at Fossil Lake, Orego 5; Toye Holmes: Miller. 22... 20.202 -c-22 2c Phase cesta ttsneneast seen eke . The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Rei . Note on a Gigantie Bear from the Pleistocene of Rancho La Brea, by John g Merriam. . A Collection of Mammalian Remains from Tertiary Beds on the Mokaxe Des by John C. Merriam. “t5 Nos.s67and. (7 in, ON COVET 2o2sces kel cecckare cntevnd sete veectctegiee Unset aoe 8. The Stratigraphic and Faunal Relations of the Martinez Formation ca ‘the Chico and Tejon North of Mount Diablo, by Roy HE. Dickerson ..................-. 9. Neocolemanite, a Variety of Colemanite, and Howlite from Lang, Los Angeles” County, California, by Arthur)S: Bakle...s:0. 32 ; 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. T yle 11. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Nort est Nevada, by John C. Merriam. Part II.—Vertebrate Faunas ............... : 12. A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, by Loye | Mi Or xo... 2ecaecndte sncnneesuectonsnatinbencnndicibesesnce saste te sug teea eens as no eee ea 13. Notes on the Relationships of the Marine Saurian Fauna Described from the Triassi of Spitzbergen by Wiman, by John C. Merriam. ~ 5 14. Notes on the Dentition of Omphalosaurus, by John C. Merriam ard Harold Cc Nos;,13sand 14.in oneacover =. ..-.2---.-- 2s eo se 15. Notes on the Later Cenozoic History of the Mohave Desert Region in in Southeaster California, by Charles Laurence Baker AI AM FHL wr 17. A Fossil Beaver from the Kettleman Hills, Galitorsia, by T dhtve Kellogg 18. Notes on the Genus Desmostylus of Marsh, by John C. Merriam ............ 19. The Elastic-Rebound Theory of Earthquakes, by Harry Fielding Reid VOLUME 7. 1. The Minerals of Tonopah, Nevada, by Arthur S. Hakle .W0...2.-.ccceececeeceo 2. Pseudostratification in Santa Barbara County, Catitorna, by George Davis Bake 2 2c5 2 22 en cbennctasasenccescedtapeee teeneecotna te pataas ate eae ae Seana ee 3. Recent Discoveries of Carnivora in the Pleistocene of Rancho La Brea, LY E7=% oh) 2s em ee ee Rap Rene FOR PU fo acre ee 4, The Neocene Section at Kirker Pass on the North Side of Mount | Mus Clark. 2!.i 82 oases, Sea tis ee ee ae sl _ 5. Contributions to Avian Palacontology from the Pacifie oast f North : Toye Holmes’ Mitier 3 eee. ee An ae eee aE ee - i UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 14, pp. 191-254, 2 text-figs., pls. 6-12 Issued April 19, 1917 THE ETCHEGOIN PLIOCENE OF MIDDLE CALIFORNIA BY JORGEN O. NOMLAND CONTENTS ees PAGE 1 rye UE a a eer 192 TETECENPATODUS) IYO) ese ea PCE oe 193 Relation of the Jacalitos to the Etchegoin ...............-.2--.2-----e22eeneeene eee eee 195 iitehegoin group of Middle California «.....-.....-..---.-.-------.2-s-scceeeceneeneceeecereeeennnencnnns 197 real distribution 20.2... Bile erie isenactil eea SEN rash Pee Nae 197 Relationysto: tadjoimin's TOLMAN a2... 2 ce ccsce ence -nineenencececeeneenctenternnernceeceeecesen 200 Relation to the Santa Margarita (?) ..-....1..-c.t.ci-10----oeeentecsteenceeneeeseneee ees 200 BEV eats TuMmaiE Oar tN MASUD ENN Gr xe ee <2 Pe Sea so Dos cy eee seen gcd obec Heese seeesteees y Ubi @ Rat © SS eee are ne sft Se ee fen ean 22M 2082 ya 22 25 seatisvenecs¥etecsde s Seedivede ss fests 2ebesa sous -actesslae é ESHEREL ADE ee Lithology of the Etchegoin Sandstone, clay, and conglomerate ...............22.-22-.0.21s:21ccsseeeeeeeeeeeeceeeeeeeeeeee 206 Woalpam dicambonaGeous: Cle 0 StS eases =- see sees eseee oes rete ces seeee sc secesseeepee eons seeecuseraes 207 BEEN O Lit Camb ites ge Fe metas Nee oer eee nee 2, Pe eee Seotees oes Seas ee es 208 CCF ONS NUE = ee one ea EF 209 GIMME SULOMC ge erence cet eee nee Sr ener Ne aR 210 HIRT INSTAL CW TALC nets CULT Geese ene feats eek ens eee Soe eR cease oa cases tees ste aeksnceceslusscueeeseese 210 TUS SHEE] OEE HE) YON ONES SY eee 0 eC 210 Etchegoin fauna west of the Diablo Range ............2..2..2..-.-2..2-----2--2---0---- 214 Wanma ‘ot Jacustrime(?): Wes oc. c.c nace ec cece cece cee eens venee eeepc tencene 215 Ram oe sOrestemmpenatune jamd «lep thy ce:::sccsessencceueeeecec- fee. -.eeeseeces2-oceeec-ceeeeceeaes 216 SSKEUTPRUUIEL (COUN), SRONCNE ry a ee eee 216 Comparative table showing stratigraphic relationship of faunal zones SOMBIE Osteen © 0 UNINC gece. eee eds Stes sce gigas ccees ee evete cee sescees sicsiel averees: tute oedeees 216 AVETALEDMALOm tani ames terse cae vee sre cts Sette elec. 2 csid ccevadace oczrvissadvaeleesssafibcens: eseciestecctacss 217 Faunal list of the Etchegoin of the Coalinga distriet -......0.20..2.022..-.--..- 218 woerand correlation Of the Htchegoin’ ......--.----cscccccssccescceseecereceseeceeeececseeeeees DOO HETHSCOy gp nOfpeCORNO] ALL OMper ee: who has shown that fossil land mammals found at the base of the lower Etchegoin (‘* Jacalitos’’) and at several other higher horizons represent the Plocene. 25 Merriam, J. C., Tertiary vertebrate faunas of the North Coalinga Region of California, Trans. Am. Philos. Soc., vol. 22, pt. 3, 1915. 1917] Nomland: The Etchegoin Pliocene of Middle Califorma — 205 It has been suggested that the Tulare may be at least in part of Pleistocene age. The Etchegoin and the Tulare have been much folded since deposition. At some localities the Tulare dips at angles of 80 degrees. This period of folding probably occurred during the time of post-Phocene diastrophic movements described by Professor A. C. Lawson.*° Since some or all of the folding took place in the Kettle- man Hills, a region of no great relief, at least 6000 feet of strata have been removed by erosive agencies. In many localities the hills have been reduced to rounded outlines and extensive terrace deposits formed to unknown depth. As the exposures are excellent and show no evidence of faulting, it is improbable that the thickness has been overestimated in the section measured. STRUCTURE The dominant structural feature of the Diablo Range in the lati- tude of Coalinga is a broad fold plunging towards the southeast. Superimposed upon this are numerous small anticlines and synclines and in some lmited areas a multitude of faults. The core of the Diablo Range consists essentially of both sedimentary and igneous rocks of the Mesozoic. The igneous rocks consist of granites and of various later basic igneous rocks of the Franciscan and later forma- tions. The sedimentaries comprise the great thickness and variety of clastic deposits which make up the Franciscan, Knoxville, and Chico. The Tertiary rocks are found flanking the main range or as remnants folded or faulted into the older series. Along the eastern slope of the Diablo Range are several anticlines branching away as spurs from the main fold. Of these the most important, in the region studied, is the Coalinga Anticline in the vicinity of Oilfields, about six miles north of the town of Coalinga, and its extension in the Kettleman Hills. Along the greater part of this area the Plocene is well exposed. The structure of the Pliocene beds flanking the main range in the Kreyenhagen Hills and north of the Coalinga is in general the eastern limb of an anti- cline. Extending along the greater part of Jacalitos Creek, the upper part of the Waltham Creek basin, and then onwards through Priest Valley and a part of Lewis Creek is a series of small anticlines and synelines with infolded Etehegoin and Tulare. This region 26 Lawson, A. C., The post-Pliocene diastrophism of the coast of Southern California, Univ. Calif. Publ. Bull. Dept. Geol., vol. 1, 1893; The geomorphogeny of the coast of Northern California, ibid., vol. 1, no. 8, 1894. 206 University of California Publications in Geology — [Vou. 10 has also been greatly complicated by numerous faults, probably due to the same compressional forces. Many of these are extensive, causing long belts of the older rocks to appear in the midst of later formations. A large number of minor faults also are present, which are too local or too unimportant to be shown on the usual geologic map. Besides the faults in a general northwest-southeast direction there are numerous cross-faults. An interesting instance of this is found in the formation of Priest Valley by the damming of the headwaters of Lewis Creek and the consequent filling with alluvium to considerable depth. The net result of the faulting has been to give the effect of a block of Pliocene having dropped down between the older formations. In the- northwestern end, a few miles northeast of Lonoak, this fault zone unites with the San Andreas fault zone, of which it appears to be a branch. At the other end it disappears in the Jacalitos syncline a few miles beyond Jaealitos Creek. In other areas of the region studied faulting since the Pliocene has been insignificant. LITHOLOGY OF THE ETCHEGOIN SANDSTONE, CLAY, AND CONGLOMERATE Due largely to the complicated distribution of the older rocks in this region, from which the Pliocene is mostly a derivative, the lith- ology of the Etchegoin varies considerably in going from one locality to another, having in the various areas a great resemblance to the kind of rock from which the sediments were derived. Also, since the formation is largely a shallow-water deposit in more or less local basins, possibly near frequently disturbed fault zones, the lthologic character has been still further localized. In nearly all instances the beds are not clearly marked off from those adjoining, but grade into each other. Few beds can be traced on the basis of hthology for more than a short distance. In the Jacalitos Hills and Priest Valley the region has been greatly compheated by faulting. South of Coalinga in the Kreyenhagen Hills the lower portion of the Etchegoin is composed of coarse, dark brown unfossiliferous sandstone. Interstratified with this is usually a minor proportion of yellowish-brown clay. Above this rests a great thickness of massive sandstone with prominent, highly indurated fossiliferous beds. At numerous horizons conglomerates occur or the beds may show their conglomeratie character only by occasional pebbles in the coarse sand- stone. Higher up in the formation the sandstone becomes of finer 1917] Nomland: The Etchegoin Pliocene of Middle California — 207 grain and more argillaceous, with a more yellowish color. Above this, or in the lower part of the upper Etchegoin, the blue or bluish- gray so-called ‘‘vivianitic’’ sandstone usually first appears. These beds do not, however, appear in all parts of the district at the same time, but in some areas extend down into the lower Etchegoin. The striking blue color is particularly well shown in the Kettleman Hills. Somewhat higher up and continuing to the top the beds consist more predominantly of clays with interbedded argillaceous sandstone. North of Coalinga the beds which have been correlated with the lower Etchegoin in the Jacalitos Hills are apparently at least in part of non-marine origin. The basal beds in this region are composed of red, brown, or gray clays. In the upper part of the lower Etchegoin the beds are more conglomeratic, consisting largely of a coarse gray sandstone with interbedded pebbles. The first invertebrate fossils appear in the lower part of the upper Etchegoin in this region. These beds are composed almost entirely of ‘‘vivianitic’’ sandstone with beds of conglomerate. Near the middle these grade into beds consisting of soft yellowish clays with argillaceous sands which continue to the top. This has been mapped as the San Joaquin Clays by F. M. Anderson.*? In Priest Valley the plane of separation of the Etchegoin from the Santa Margarita (?) below has not been definitely determined. All the lower part of the formation is nearly devoid of diagnostic fossils. These beds as a whole, up to the middle of the upper Etche- goin, are characterized, however, by a brown sandstone of medium texture with only a small proportion of conglomeratiec material. Above this the deposits grade into a predominantly fine-grained shale and clay, with a large amount of interbedded coal and carbonaceous material. From here up to the top of the Etchegoin the yellowish- brown or grayish, rather coarse-grained sandstone is the most evident. Fossils indicative of middle Etchegoin have been found on the west side of the Diablo Range near Lonoak, Monterey County, Cali- fornia. These fossils are imbedded in a thick series of beds composed largely of lght-colored shale and voleanie ash. The rock is fine- grained, with only a very small proportion of coarse arenaceous material. COAL AND CARBONACEOUS DEFOSITS Carbonaceous shale and beds of coal occur at various horizons of the Etchegoin. A seam of coal was found in what apparently are 27 Anderson, F. M., A stratigraphic study in the Mount Diablo Range of California, Proc. Calif. Acad. Sei., 3d ser., vol. 2, no. 1, 1905. 208 University of California Publications in Geology — [Vou. 10 beds of lower Etchegoin on Frame’s ranch, in the upper region of Jacalitos Creek. On one of the branches at the head of Waltham Creek thin beds of carbonaceous material were found near the middle of the formation. The coal deposits in the Etchegoin of Priest Valley, however, are by far the most important both in thickness and areal extent. This area has already been mapped and lithological sections given by Robert W. Pack and Walter A. English.°* As indicated by these deposits, it seems possible that the Etchegoin in Priest Valley and adjacent areas may have been laid down in a basin connecting the sea in the Great Valley with that west of the Diablo Range. That such connections probably existed has already been pointed out by F. L. Ransome,*® who states: ‘‘The Great Valley was probably occupied during the whole of the Neocene by a gulf, connecting with the ocean by one or more sounds across the Coast Ranges.’”’ RHYOLITIC TUFFS Effusive rocks have been found at three horizons in the Etchegoin. These consist of rather persistent tuffaceous bands interstratified with other rocks of clastic origin. From the uniform thickness of each bed, the stratification planes often being distinetly visible, and from the intimate relation to strata containing a marine fauna, it is evident that these rocks were deposited in the waters of a shallow sea. The fine, well-sorted character indicates that the voleanie action must have taken place at a considerable distance from this area, although prob- ably in the Diablo Range, along the foothills of which the Etchegoin outcrops. On approaching Jacalitos Creek from the Stone Canon coal mine to the west a prominent white bed or band ean be seen on the eastern bank several miles before reaching the creek. This is the lowest of the three horizons indicative of voleanic action in the Pliocene of this region. The bed is about twenty feet thick and is exposed for nearly two miles along the strike until cut off by faulting. Petrographie examination shows that quartz and orthoclase feldspar are the pre- dominant minerals in this rock. Plagioclase feldspar is also present, but in minor proportion. The composition therefore corresponds to that of a rock usually grouped under the term rhyolitic tuff. 28 Pack, Robert W., and English, Walter A., Geology and oil prospects in Waltham, Priest, Bitterwater, and Peachtree valleys, California, U. S. Geol. Surv. Bull. 581D, 1914. 29 Ransome, F. L., The Great Valley of California, a criticism of the theory of isostasy, Univ. Calif. Publ. Bull. Dept. Geol., vol. 1, p. 386, 1896. 1917] Nomland: The Etchegoin Pliocene of Middle California — 209 A few miles east of the bed last deseribed, or about five miles south- east of Coalinga, another band outcrops on the west side of the higher hills. This bed resembles very closely in texture and petrographic characters the tuffaceous material on Jacalitos Creek. These charac- teristics, together with faunas of middle Etchegoin age collected above and below each of the two bands, indicate that they probably belong to the same horizon. Closing the period of deposition of the marine Etchegoin, or im- mediately before the transition of these beds into the prevailingly terrestrial deposits of the Tulare, voleanoes were again active in this region. This is shown by the large proportion of tuffaceous material mixed with the clays of the Mya japonica zone of the north Coalinga region. The tuffaceous material is of very fine texture and of rhyolitic composition. At one locality about one hundred feet stratigraphically below this horizon another bed of tuff has been found. This material is rather coarse-grained, as if deposited and later broken into frag- ments and redeposited. The tuff in this band is interstratified with a large proportion of quartz sand. The tuffaceous beds of the upper and lower Etchegoin, being usually very persistent, should prove of value for correlation purposes if found in other parts of the field. The striking characteristics of the beds make them readily distinguishable even at a considerable distance. It appears rather remarkable that they have not been found in the Kettleman Hills and in the Kreyenhagen Hills, a few miles to the south. GYPSUM At several horizons of the Phocene in this district large quantities of gypsum have been found. In no instance, however, except near the base of the Tulare formation, are these beds known to be inter- stratified with the clastie series. At that horizon on the eastern flank of the Kettleman Hills thick gypsiferous beds oceur with extremely fossiliferous fresh-water deposits. At several horizons in the Etche- goin large quantities of gypsum are found. Since these deposits of gypsum usually are in a very fragmentary condition, they cannot be assigned definitely to an origin contemporaneous with that of the beds. It seems improbable that large quantities of gypsum occurring exten- sively only at definite horizons could have filtered from other sources into fissures and cavities subsequent to the deposition of the Etchegoin. Gypsiferous beds are probably not deposited under normal marine 210 University of California Publications in Geology — [Vou. 10 conditions. It is believed, therefore, since such conditions undoubt- edly frequently obtained in the Etchegoin, that the beds of gypsum were deposited, at least in part, in basins isolated from the ocean, in fresh-water lakes, or on a periodically flooded delta at the time of deposition of the Etchegoin. The climatic conditions under which this deposition took place were probably arid. LIMESTONE Along the divide between Jacalitos Creek and Salt Creek, about one-half mile east of Robert’s ranch-house, a limestone bed outcrops. On megascopical examination the bed is found to be compact and massive in the middle, but the upper and lower portions are lami- nated. These laminae are very thin, being not over 2 mm. in thick- ness. On examination with a petrographical microscope a few minute grains of quartz were observed. The bed both above and below grades into sandstone typical of the formation. It has a thickness of about ten feet and is traceable about one-half mile until intersected by faults. With coarse sandstone above and below containing fossils indicative of a shallow marine origin, the conditions necessary for deposition of limestone in the ocean were probably not present. The conclusion is therefore reached that the limestone may have been deposited under some such conditions as might obtain in a temporary lake, or in an estuary temporarily severed from the sea. INVERTEBRATE FAUNA INVERTEBRATE ZONES Four distinct faunal zones have been recognized in the Etchegoin. No fossils have been found near the base of this group. The lowest important fossiliferous horizon is the Chione .elsmerensis zone, in which C. elsmerensis English is abundant. This faunal association extends through several hundred feet of strata in the middle portion of the lower Etchegoin and is typically that of the lower Etchegoin, or ‘‘Jacalitos,’’ as deseribed by Arnold and Anderson. Several of the species are unknown outside of this area. The occurrence in these beds of C. elsmerensis English, C. fernandoensis English and several other forms shows that its closest correlative is found in the lower Fernando near Newhall, Los Angeles County. The typical faunal assemblage of this zone may be found at locality 2526. Among the characteristic species may be mentioned Astrodapsis jacalitosensis 1917] Nomland: The Etchegoin Pliocene of Middle California 211 Arnold, Chione elsmerensis English, Chione fernandoensis English, Dosinia jacalitosana Arnold, Macoma vanvlecki Arnold, Paphia jacalitosana Arnold, Chrysodomus portolaensis (Arnold), Margarita johnsont Arnold, and Thais kettlemanensis Arnold. LIST OF INVERTEBRATES FROM THE ‘‘JACALITOS’’ OR LOWER ETCHEGOIN, WITH OCCURRENCE AT OTHER HORIZONS s il ee & ie cs 5 2 & @ & RQ n a fa ECHINODERMATA Astrodapsis jacalitosensis Arnold ........................ Astrodapsis peltoides Anderson and Martin ...... MSS AECOXG EH OFSHSP 8a 1S) Ope eeegeer tree errr Dendraster gibbsii (Rémond) ~.............2-.2..2--2.------- awe gees x Dendraster gibbsii, n. var. B -......222022.2-222---- Dendraster coalingensis Twitchell -.........2..2..22.....- PELECYPODA ANenlley (ce lshagerasis) (AaGheKCls))) See ee ee see x x Anca brulimeatas © oma ecsseccces so 2eeese:seeeceseeceseeeee ee x Cardium quadrigenarium Conrad ................2.------- x x x x Chione elsmerensis English -.................22-.-22.--------- Chione fernandoensis English ...............-..-..--.--.-- ee Cryptomya californica (Conrad) ............-.....----- 2 2 x x Cryptomya quadrata Arnold ~........2..2.--2-2e Cumingia californica Conrad ...............2-22.212---- Seo Pee ee x Cyrena californica Gabb ..............2..-2-.-.-2---------o- = x Diplodonta parilis (Conrad) -..........--...-------.------ ae x x Dosinia jacalitosana Arnold ..........2..21..22.22::220020--- Glycimeris coalingensis Arnold —.........-.---.--.------ es x x Glycimeris septentrionalis (Middendorf) .......... oe x x Were dayact step irda) eile sse eee ceases ccsee te eese eens eee ee x Macoma baltica (Linné) ........202..220.222.22----- ee Macoma jacalitosana Arnold ...............------------2------ Macoma nasuta (Conrady) sce -cccceeceeeerceeeeecse x x x x Macoma secta (Conrad) ............--..21----22-0--eeeee eee x Macoma vanvlecki Arnold ............-...2.----.2----2--------- Metis alta (Conrad) ...............- FR trae Pda rare x ar x Miodwolws rectus: Commadl 2s.2sc.2eces.eeceete see cveceeec ees x x x Monia macroschisma (Deshayes) .........----.------------ ee Ge es Xx Mnnlimay dlensart a@ oma Cie eee eee x Mytilus coalingensis Arnold ..........20.02---.-------- 2 2 Mytilus kewi Nomland ........ Beppo eer eee x @strea rat woods Gas sss secs cece sce seeee ce sceeeerce recess = x x Pandora, punctata Conrad 222222 ee x x anope -cenorosay Groulld)) aie. sce aca eam eaee ee weee eee x x x x 212 University of California Publications in Geology — [Vou. 10 LIST OF INVERTEBRATES FROM THE ‘‘JACALITOS’’ OR LOWER ETCHEGOIN— (Continued) ¢ 6 «a8 &« Rh al : fC Paphia jacalitosensis Arnold ie gee PRaphiarstamaimes: (Connaid))eescce recess eee x ? x Paphia tenerrima (Carpenter) ............2....22-.2-22----- x x Pecten etchegoini wattsi Arnold ........................- ae x Pecten (Hinnites) giganteus (Gray) -................- x x x iRecuem, heale ya Acero dieec:cssssse cette states ceeeteeeee sense x Becton owena Arm ol disses seers ereesece senses eee ese x Pectem terminus, Aco dl ee rece.ccet ceo esesreeeesesseeneae = Xe Periploma argentaria Conrad .......21..2..22:.-2::2:000++- x Phacoides annulatus (Reeve) --....-...--..---ce----tess---- x x x x Phacoides richthofeni (Gabb) x x x Psamobia edentula (Gabb) -.............. — x Sanguinolaria nuttalli Conrad x x Saxidomus nuttalli Conrad -....022.22.002220222.---1e----- x x x x Schizothaerus nuttalli Conrad .......202.222...----------- x x x x Rak Sudo} (=YiGat | © Pale pet eg ee ae Ue cee Siliquamlicud ay (Comma c)) geese seeeseeeserreetes: eee ae ae rr x MOLems SIC amI Sis GO Cleese ee eens eee ae x x Spisuilay alli ama eC ommerdy) ese. eeeterese ee eee x x x Spisula coalimgensis (Arnold) esse ecc.cccec eee eaee Zit ees X ogy Fe Spisula hemphilli (Dall) -.......2.22222222-22-22--2--2--2------ ae x Melina ode sensrs ai Sie cceceecerereee seers teee eee sade ee Ee x Thracia jacalitosensis Arnold Tivela trigonalis Nomland ................2.2-2..22---22------ see ees x PVONCTANCO OP eri Gra NN eae eee x ae tee x /Aroe olabeveres Cehtsy oye (VU rnAWENe)) Sages ers ee yess Diptee x GASTROPODA AStralium yarn oldie Niomil amid secre cee ceeeee se eee serra Calliostoma coalingensis Arnold ....................--.- eet eee x Calltostomas kerry sAmmo) eee eern seen etree reeereees ees x Wallyjptraeaetilosem (Grail) meeccesee ene nere ce eres x > x Cancellaria fernandoensis tribulis, n. var. -......... Cancellaria crassa, mM. Sp. ----2-.---2222.--s:sse-0- PeSRah Chrysodomus coalingensis Nomland ................... Ses eee, Se Chrysodomus imperialis: Dall 22s a g x Chrysodomus packardi, 0. SP. ........2-.22..2200eeeeee ‘ Chrysodomus portolaensis (Arnold) .................. eee ees x Crepidulasadim cae Owen syn crecesrcce eee ae es ek x Crepidula, princeps’ Conrad 222i serene x x x BD WeOhoNsy satay tse KopDish (CG 0) 0) eet eee x x x Fissuridea subelliptica Nomland ..........-.....-. -. Margarita johmsoni Arnold) .2...2...2::222:.:tssececcseseseee Zeca eee x WW hubifeb'e Coro aVCr babies Ue SO eee eee rere 1917] Nomland: The Etchegoin Pliocene of Middle California 213 LIST OF INVERTEBRATES FROM THE ‘‘JACALITOS’’ OR LOWER ETCHEGOIN— (Concluded) s S bi ica a Nn oI = 4 Murex perangulatus Nomland .~........................... Murex tethiys, nm. sp. -22--22 sual SEE Nassa californiana (Conrad) x Natica orbicularis Nomland x Naitrcarmecluizanas Petit (esse esc x x x x Olivella biplicata Sowerby —.............22.--2.--22..0------- ey ne * x Jequiigoybaey qrvbeiatsy IN oper Wish eKsl Pay yess ere eey ee eye xe Sinum scopulosum (Conrad) ...........----2.-----.--------- x x x Thais kettlemanensis Arnold ................2..-.....-..-- St bg x Thais lamellosa (Gmelin) —........00-2.00.--2.2-2------------ ae gee x Trophon belcheri avitum, n. var, ........-....---.--------- Trophon coalingense Arnold x Trophon magister Nomland x Turris carpenteriana (Gabb) Turris coalingensis (Arnold) -............2.-22..22.-20-2-+-- L220 2S x AUDITS Tay onanichote), (CGY 6 a))) | eee ee eee epee aes, pate © hext x Turritella nova Nomland ..........0..022---- eee CIRRIPEDIA IB¥albhannls} Cover hwailss IBhtopaal eee ee Sn x x Tamiosoma gregaria Conrad ........0...2-.2----12ee eee iol ks x At a number of localities in the Jacalitos Hills and Kreyenhagen Hills in beds of the lower middle Etchegoin a faunal assemblage has been found characterized by several species unknown at other horizons of the formation. This fauna, known as the Turritella nova zone, is found typically developed at locality 2533. At this station the fauna consists of very large specimens of Pecten owent Arnold, Pecten terminus Arnold, and Phacoides annulatus (Reeve). Well-preserved specimens of P. terminus may be found which have the very unusual width of 145 mm. Associated with these species are numerous gas- tropods such as Ficus nodiferous Gabb, Turris carpenteriana (Gabb), Turris tryoniana (Gabb), and Turritella nova Nomland. The most easily recognizable by its faunal assemblage and the most persistent in areal extent in the Etchegoin is the Pecten coalingensis zone. The name was first apphed by Arnold to a zone occurring in the Kettleman Hills and in the Jacalitos Hills about 800 feet below the summit of the formation. Subsequent work by the writer has shown that this faunal association, occurring at approximately 214 University of California Publications in Geology (Vou. 10 the same horizon, is also found well developed in the Priest Valley, and that it is present north of Coalinga in beds traceable to the type section of the Etchegoin of Arnold and Anderson. At all localities where this association is found the stratigraphic range of the fauna appears very short, and there is no repetition at other horizons of a similar assemblage. A strikingly large number of the species are unknown outside this zone. In it are found a coral, a brachiopod, several species of Pecten unknown in other horizons. One of the most characteristic forms is Pecten etchegoini Anderson and its vari- eties nutter? Arnold and watts? Arnold. It has been found that this species, which has been used largely for correlation in the Pliocene, has a very long range. This form occurs south of Coalinga from below the Turritella nova zone to the uppermost beds of the Etchegoin group, or approximately through 4000 feet of strata. Trophon ma- gister Nomland, formerly thought of very limited range, has been found in this zone. A number of the more recent forms are also rarely found, such as Pecten hastatus, var. hindsi Carpenter, Murex festivus Hinds, Trophon gracilis (Perry). Uppermost in the predominantly marine deposits of the Etchegoin and directly below the fresh-water deposits of the Tulare a faunal assemblage is found which has been named by Ralph Arnold the Mya japonica zone. It is found persistently in the Kettleman Hills and in the Kreyenhagen Hills. North of Coalinga a similar fauna has been found in a resistant band of argillaceous tuff in the outer- most foothills. In Priest Valley the zone does not occur and the line of demarcation between the Etchegoin and the Tulare is distinguished with difficulty. The fauna of the uppermost part of this zone is mainly that of shallow-water or littoral conditions. A number of species found immediately below the typical Mya japonica zone at several localities are included with the fauna of that zone in the accompanying list. The only species of this zone unknown in other horizons is Littorina mariana Arnold and its variety L. mariana, var. alta Arnold. In most of the localities along this zone the so-called fish bulbs are found in large numbers. North of Coalinga the extinct horse Pliohippus proversus Merriam is found at this horizon. ETCHEGOIN FAUNA WEST OF THE DIABLO RANGE It has already been stated that the Pliocene is present on the west side of the Diablo Range in the latitude of Coalinga. The following Pliocene species have been obtained on the north bank of Whalen 1917] Nomland: The Etchegoin Pliocene of Middle Califorma 215 Creek a short distance above its junction with Stone Canon and on Big Sandy Creek about one-half mile above its confluence with Stone Cafon, near the southeast corner of Priest Valley Quadrangle. Fauna From Big SANDY CREEK AND WHALEN CREEK Dendraster gibbsii (Rémond) Pecten healeyi Arnold Cardium, cf. quadrigenarium Conrad = Phacoides, sp. Cryptomya californica (Conrad) Schizothaerus nuttalli (Conrad) Macoma nasuta (Conrad) Siliqua lucida (Conrad) Mulinia densata Conrad Solen, ef. sicarius Gould Ostrea, sp. Zirphaea, sp. Pandora punctata Conrad Calliostoma, sp. Paphia, sp. Chrysodomus, sp. Paphia, cf. tenerrima (Carpenter) Nassa californiana (Conrad) Pecten estrellanus catalinae Arnold Natica recluziana Petit About one and one-half miles southwest of Lonoak post-office, Priest Valley Quadrangle, the following fauna indicative of the middle Etche- goin has been found. The fossils occur in a series of beds of fine white ashy shale, extensively distributed in this area. Fauna From LONOAK Cryptomya californica (Conrad) Fissuridea, ef. unica, n. sp. Ostrea atwoodi Gabb Natica, sp. Pecten oweni Arnold Trophon, sp. Pecten estrellanus Conrad, var. Tamiosoma gregaria Conrad Also on Vineyard Creek, San Luis Obispo County, and Indian Valley, Monterey County, west of the Diablo Range, Etchegoin sand- stone and conglomerate overlying Santa Margarita shale is extensively distributed. The included fauna is apparently of lower Etchegoin or 5) ‘* Jacalitos’’ age. FAUNA OF LACUSTRINE(?) BEDS In the north central part of the Kettleman Hills, near the middle of the southern part of sec. 12, T. 22S, R. 17 E, M. D. B. & M., a bed containing fresh-water fossils was discovered recently by the writer. According to its location with respect to the upper Mulinia zone as mapped by Arnold and Anderson this bed comes only a short distance above what is called by them the base of the Etchegoin. This would therefore come at about the same horizon as is represented by the unconformity recently deseribed*®® in the region north of Coalinga. It appears that the time-interval marked by the unconformity of 30 Nomland, J. O., Relation of the invertebrate to the vertebrate faunal zones of the Jacalitos and Etchegoin in the North Coalinga Region, California, Univ. Calif. Publ. Bull. Dept. Geol., vol. 9, p. 80, 1916. 216 University of California Publications in Geology (Vou. 10 the northern area is indicated by fresh-water deposits in the Kettle- man Hills. Although fossils are very abundant in this bed, only the following forms could be identified: Anodonta nitida, n. sp., Goniobasis, sp. RANGE OF TEMPERATURE AND DEPTH As shown by Ralph Arnold, the temperature of the ocean during Etchegoin time was probably somewhat warmer. than that of the Pacifie Ocean in the latitude of Coalinga at the present time. A large number of the Etchegoin forms, with other species indicative of decidedly warmer water, at present live from Monterey to San Diego. The large specimens of Pecten terminus Arnold are indicative of warm conditions. Metis alta (Conrad) and Periploma argentaria Conrad found in the lower Etchegoin indicate warm water. No cold-water phases have been recognized. The invertebrate fauna of the Etchegoin is composed entirely of forms living in shallow water. At some horizons, loeally, forms char- acteristic of brackish or even fresh water are present. Species char- acteristic of considerable depth have not been found. SERPULA(?) REEF In beds of middle Etehegoin in the Krevenhagen Hills, on the south bank of Garza Creek, see. 35, a reef outcrops which is made up almost entirely of tests of the genus Serpula(?). This reef is exposed along the hillside for about thirty yards, with a thickness of about one and one-half feet. COMPARATIVE TABLE SHOWING STRATIGRAPHIC RELATIONSHIP OF FAUNAL ZONES SOUTH OF COALINGA Arnold, 1910 Faunal zones Mya Pecten coalingensis Upper Mulinia Glyecimeris or Lower Mulinia Middle Big Trophon Nomland, 1916 Faunal zones Mya Pecten coalingensis Turritella nova Chione elsmerensis Arnold, 1910 Formation Etchegoin Unconformity Jacalitos Unconformity (?) Santa Margarita (?) Nomland,. 1916 Formation Etchegoin Unconformity Santa Margarita 1917} Nomland: The Etchegoin Pliocene of Middle Califorma 217 VERTEBRATE FAUNA Perhaps the most interesting and valuable material for purposes of correlation found in the Etchegoin is represented by the remains of land mammals occurring at many widely separated localities. This material has been found at several horizons in both the upper and lower divisions of this group. The most important of these occurrences is about ten miles north- east of Coalinga. In that area in both the upper and lower Etchegoin vertebrates are found in zones with invertebrate zones or alternating with them. The vertebrates from this area have already been de- seribed by Professor J. C. Merriam.** indicates other formations in which the species is found.) 1917] Nomland: The Etchegoin Pliocene of Middle California 219 FAUNAL LIST OF THE ETCHEGOIN OF THE COALINGA DISTRICT— (Continued) zy leas 28 22 88 See og CS ape eS A of « &§ 3 04 2 pw Bi Peet jac pet SIN + SB Fa Gwe ss Se sw Bods cn S Diplodonta parilis (Conrad) ................ Cc C Dosinia jacalitosana Arnold ~.............. Cc oa x Glycimeris coalingensis Arnold .......... C Cc x : Glycimeris septentrionalis (Midden- 2... 22.0 2. lee ee X LON Ls) ecco cne Sess cee eeeeecceeeeeictees ees sveeices Leda, cf. taphria Dall -.....22.... ee, gates Macoma baltica (Linné) ...................... es ee oo cee Macoma inquinata (Deshayes) .......... Cee CeCe Coo xe. XxX Macoma inquinata affinis, n. var. -..... ee Macoma jacalitosana Arnold .............. UR = : nee Macoma nasuta (Conrad) —......2-2..---.- Coe Cee xX EX Macoma secta (Conrad) ...........-...-.-.--. ee ere ae x Macoma vanvlecki Arnold .................- Ce ee Metis alta (Conrad) <.........--.---:e--eeeeee- Ces x Modiolus fornicatus Carpenter .......... pee Se LR ee eer este ee aes: x Modiolus rectus Conrad .......222...2.-2-..---- COC CER ee eee x % Monia macroschisma (Deshayes) ...... G Cc .. x Mulinia densata Conrad .....................- CC eee eS. ee CBee IMD), PTOLONINCRY Be ec eee cme XA eins Dees Peds OX Mytilus coalingensis Arnold ................ ee xX x Mytilus kewi Nomland ...........20.2........- seis, ais, Poss Ostrea atwoodi Gabb ........2..22.222..2..---.- Cc C C x Ostrea lurida Carpenter .....................--- C OC x Ostrea vespertina Conrad .................... Cc OC Ostrea vespertina, var. sequens Arnold Cc OC Pandora punctata Conrad .................--- es tees Nee a Panope generosa (Gould) -..........2.....-.. Cc C C xox x Paphia jacalitosana Arnold ................ LE Sg Sea ee ere re er Paphia staleyi (Gabb) -...2..0.20..2.....-- ee ee ee = Paphia staminea (Conrad) ...............-.- CC ee ES a Cn 2 Paphia tenerrima (Carpenter) -........... CD ere Xe ee OE Xr OX Pecten coalingensis Arnold ................ oe URG: Pecten egregius, n. Sp. -.--.------.---cecceeceeo- ee UR neon fears Pecten etchegoini Anderson ................ eee © eee SX Pecten etchegoini nutteri Arnold __.... Ears NS OF ence Sees ove Pecten etchegoini wattsi Arnold ......... pee Wey Meee Meas 2X Pecten (Hinnites) giganteus (Gray)... = Pecten hastatus hindsii Carpenter ._.... Se eS cee er eee Pecten healeyi Arnold -.....02.2....-0.0.-- eee aera x Pecten oweni Arnold -.........22..:::0----- Co Ce ee xX x Rectem proteus, tM. Sp. -.-cceccee--cee-e-e ee UIC Pecten terminus Arnold 0.00002... C OC (C indicates that the species is common; R indicates that the species is rare; U indicates that the species is unknown outside of this horizon; % indicates other formations in which the species is found.) 220 University of California Publications in Geology (Vou. 10 FAUNAL LIST OF THE ETCHEGOIN OF THE COALINGA DISTRICT— (Continued) ze Be § 23 2s $2 fe sf sh ye a eh 3 ae 5388 82 66 be Sa 5 Sauee Sse ee ea So Sy fe Periploma argentaria Conrad ~............. aes x Petricola carditoides (Conrad) .......... R = x Phacoides annulatus (Reeve) .............. fle. “Qe 0a XK XOX See ae Phacoides richthofeni (Gabb) ............ R x Phacoides sanctaecrusis Arnold .......... fetes | oe eee Pholadidea ovoidea Gould .................... weve seal, (SSL ah 28h, Placunanomia californica Arnold ...... weed, dacs “Uaees east Ei, LG. SESE eee Psamobia edentula (Gabb) —................ en G8) aks) 2a OG 2 ~eee Psephis ordi (Baird) 2s Secs ceecussscesoes ws Jae ae a PES 2 Sanguinolaria nuttalli Conrad —........ Wi eR 623 Gee dete) cee oe Saxidomus nuttalli Conrad -... = Cea x x Schizothaerus nuttalli Conrad ~.......... Co (0 Gas 2 22 OS =X. xe aa Demele: Tausta, ems Spy eee seeeee erence wot) aoe UR Ate See ee, 2 ee Semele rubropicta Dall 22 oe. gsm, WER SSS 128) eX ee Suiliqua: Iuecirda (Conrad!) 2222-222. cess CP Ohh. Ge. eee x Solen sicarius Gould ...22.......22.--------------- Ge wan 2. (OOO KIX xX Cea ae Spisula albaria (Conrad) ... Xx ™M®: X Spisula coalingensis (Arnold) —.......... wis this [cc 2 ee EX, a eee Spisula falcata (Gould) —.................... _ Pee er ih Spisula hemphilli (Dall) -.....-........... Ue ek ee Sa a en x Tellina bodegensis Hinds .................... CS eek ee ee ea ene Tivela trigonalis Nomland ..... a oe Mhracia LOPMIOSa,, Wes Ps s..cssseeeeeeeeee == Wes ooze Thracia jacalitosana Arnold ................ Transennella californica Arnold ........ sire Sages 2 Blac Woldiacooperi: Gabi eee sites aise nee OD SX ee x Zirphaea crispata (Linné) ................-- fess desu pace, , Geccg ess eae x GASTROPODA Astralum arnoldi Nomland ................ = . Calliostoma coalingensis Arnold ... Ca Cane x 3 : é Calliostoma etchegoinensis Nomland .. - y Calliostoma kerri Arnold ...............--..--- i a © 23 a 25 225 Calyptraea filosa (Gabb) -.................---. C we CGC °C. x << eae Cancellaria crassa, 0. SP. -..-...--------------- oan (Olee < : Cancellaria fernandoensis tribulis, n. AE ee eee Pree Wanicelllariammapal, Mts) tess eeene eee : Bee Cancellaria tritonidea Gabb ~............... ia eee CR 2 ss A ee Chrysodomus coalingensis Nomland .. : Chrysodomus imperialis Dall -............. R of ee (C indicates that the species is common; R indicates that the species is rare; U indicates that the species is unknown outside of this horizon; % indicates other formations in which the species is found.) 1917] Nomland: The Etchegoin Pliocene of Middle California FAUNAL LIST OF THE ETCHEGOIN OF THE COALINGA DISTRICT— (Continued) Chrysodomus packardi, n. sp. —--.-...--.- Chrysodomus portolaensis (Arnold) Columbella (Astyris) richthofeni Gabb Crepidula adunca Sowerby ................-- Crepidula princeps Conrad —..........-.- Drillia mercedensis Martin ~............-.. Epitonium varicostata Stearns ........ Ficus nodiferous Gabb ................--------- Fissuridea subelliptica Nomland ........ Fissuridea unica, n. Sp. ....-.-...-------------- Goniobasis kettlemanensis Arnold .... Littorina mariana Arnold .................... Littorina mariana alta Arnold .......... Margarita johnsoni Arnold .................. Miaurex COmcCinma, Ms SPs 2-22. ..se2es--2-ce--c=-- Murex festivus Hinds Murex perangulatus Nomland ............ Murex tethys, n. Sp. .....-2--2-.22:22:22:--0----+ Nassa californiana (Conrad) _ Natica convexa Nomland —............. Natica orbicularis Nomland Natica recluziana Petit -....................... Natica recluziana alta Dall -............. Olivella biplicata Sowerby -................. Olivella pedroana (Conrad) ....... Pisania fortis angulata Arnold .......... Purpura turris Nomland ~..................... Sinum scopulosum (Conrad) ..............-. Tegula (Chlorostoma) pulcella, n. sp. -. Thais kettlemanensis Arnold Thais lamellosa (Gmelin) —.................. Trophon belcheri avitum, n. var. ...... Trophon coalingense Arnold ............. Trophon gracilis (Perry) ...................- Trophon magister Nomland Turris carpenteriana (Gabb) Turris carpenteriana fernandoana PASTE Ol Cl yeahs cece) sees cscs season eres, 82s Turris coalingensis (Arnold) Turris tryoniana (Gabb) —................. Turritella nova Nomland 0... Turritella vanvlecki Arnold ................ Chione elsme- gensis zone C 2 UC . UC _ UR Em zi =| Ce 3c C Cae UR C Cae CLG Cc CO ? Cac Cevae .... UR R ? CC C RC Cc UC, os ‘S ° i) yo a) 3 a 5 = rst Ss Ss Hus o se HO "2O OF Bo 2 oO pe eh Ae as caus ¢ 5 ES gs Se wal ee oF = KH | x x x x CO x x x 4 x fi! C x x re MS cece x e \ 4 ne fa ‘ Cee ee x x x x "4 221 Recent (C indicates that the species is common; R indicates that the species is rare; U indicates that the species is unknown outside of this horizon; X indicates other formations in which the species is found.) 222 Umwversity of California Publications in Geology — [Vou. 10 FAUNAL LIST OF THE ETCHEGOIN OF THE COALINGA DISTRICT—(Concluded) 2» Ze § 5 i=} oR & eI ° as 8 88 8 = OO og n ON n & 3S va 5 I co) Da a4 3 fy SO FL Omm ames ORES F2 Ee Sete SE Sh BR 2 5E ge 52 82 52 32 33 of ooeecmee ; Or 2 a SN Se Se Sa 3 CRUSTACEA Balanus coneavus Bronn ............0......... 2 CG IC, an 2 eo Cancer fissus Rathbun .........200....222.....- sisi adesi9 acta) ssned aete “ly ee rn Loxorhynchus grandis Stimpson .. : : ee Tamiosoma gregaria Conrad ................ Clo it ee cn. (a5. PISCES Carcharodon arnoldi Jordan ................ He Ove, Ri EO aes) Gi ne Fish, bulbous growths ese ito eee REPTILIA MGS hid OC 2i)eS po esieceeesesessseesese cee vsds >, Sale ecetey Seen ae MAMMALIA Camelops or Pliauchenia, sp. .............. ee anh) Ae Se ee 22h Ee Castor californicus Kellogg ................ wii» GE Tie, yeiee Bern (ies esos gee a ns Cervus or Odocoileus, sp. ........-..-..-.------ dees gist tee ates acres oy ee en DWV LENS Roe (oj oY eet ee nla ona ee ee if eRe. Sse ke AS Een ee eee Neohipparion molle Merriam 2 Pliohippus coalingensis’( Merriam) 2.2 222 2.0 222 2 2s a ee Phohippus proversus Merriam ............ tise, Gad ae eae a 2 ee Plohippus; ef, tejonensis) (Merriam))\2 22.) 2 eee eee eee eee eres eee leanayeron elvis iy 0%) cece eee eee cudtWy uwise, Messe) eesz, Secon gece (ee Mary assis or Wty ob ys jesesseeee saree tow Mi eee? EE. Geuy She. See rs (C indicates that the species is common; R indicates that the species is rare; U indicates that the species is unknown outside of this horizon; * indicates other formations in which the species is found.) SUMMARY OF ETCHEGOIN INVERTEBRATE FAUNAL LIST WaT) 0 0.0) ee ee a a a eee il PiGhinoderNVatal, Fcc secede codes cpscveeacseezceeeseceevew« Sbecessectve sesso seesoe se eee ee 11 Bf 216) 60 GY 6 nem Re Peer eee Sere 2 Pelecy oder. 25 es8 ce cose cece ee os See SE 80 CG oH 50) CLO 6 Va ar ee eee BaP PR EO Orn RE rere PET er AE ie, 53 @TUSt aC ears sae ee ea eee ans ee ee 2) eee 4 Total number of determinable Etchegoin invertebrate species —..................-- 149 Number of Recent molluscan species in the Etchegoin -......20.. eee 50 Percentage of Recent molluscam Species <22...2c2sc.cecsceccccceeteectesncreecsenseeeeee eee 39 Percentage of Recent species in gastropod fauna of Etchegoin 21 Number of species known only from the Etchegoin of Coalinga 42 Total number of species reported from the lower Fernando near Newhall ... 60 Number of species common to the Etchegoin and the lower Fernando near Nie spy bel occa cscs execu cc cce ee cescs vce cane cae tebe eee ons ree ca en ne nee 27 Total number of species reported from the lower Pliocene near Sargent ...... 38 Number of species common to the Etchegoin and the lower Pliocene beds BU 64 Toy Ur OT ites en eee 30 1917] Nomland: The Etchegoin Pliocene of Middle California 2238 Total number of species reported from the upper Pliocene near Sargent ... 45 Number of species common to the Etchegoin and the upper Phocene beds FING ATS AE OT Gace eee ese see teas as Se ee carrer Meera cnn ee nro wemcgee ote Jerez eter genset e222 Seer 26 Total number of species reported from the Purisima -........--.------------------ 59 Number of species common to the Etchegoin and Purisima —......----------- 32 Total number of species reported from the lower Merced .................-.------------ 41 Number of species common to the Etchegoin and lower Merced ...............-..-- 25 AGE AND CORRELATION OF THE ETCHEGOIN HISTORY OF CORRELATION The name Etchegoin Beds, used by F. M. Anderson** in the first descriptions of the formation, included only the upper Etchegoin as used by the writer. These beds were thought by Anderson to be of approximately the same age as the San Pablo formation, this corre- lation being based chiefly on lithology. The Etchegoin Beds and the San Pablo were both included in the Pliocene. The thick series of strata immediately underlying the Etchegoin Beds, including the Jacalitos, Santa Margarita and a portion of the Vaqueros as later mapped by Ralph Arnold and Robert Anderson, were grouped by F. M. Anderson as the Coalinga Beds. These beds were believed to be of upper Miocene age and to be separated from the Etchegoin Beds by an unconformity. The Jacalitos and Etchegoin formations as mapped by Arnold and Anderson*® were held to represent the middle and upper Miocene. The Etchegoin was considered equivalent to a considerable part of the San Pablo. The Etchegoin was also believed to be equivalent to, or possibly older than, the Purisima and was thought to be earher than the Mereed. According to Professor J. P. Smith,*° ‘‘The lower division of the upper Miocene consists of the San Pablo-Santa Margarita-Jacalitos faunas, which are a unit, or nearly so... the Jacalitos being merely the upper division of the Santa Margarita, and both together being 34 Anderson, F. M., A stratigraphic study in the Mount Diablo Range of California, Proc. Calif. Acad. Sei., 3d ser., vol. 2, no. 1, 1905; A further study in the Mount Diablo Range of California, Proc. Calif. Acad. Sci., 4th ser., vol. 3, 1908. 35 Arnold, Ralph, and Anderson, Robert, Preliminary report on the Coalinga Oil District, U. 8. Geol. Surv. Bull, 357, 1908; Arnold, Ralph, Palaeontology of the Coalinga District, Fresno and Kings counties, California, U. 8. Geol. Surv. Bull. 396, 1909; Arnold, Ralph, and Anderson, Robert, Geology and oil resources of the Coalinga District, California, U. S. Geol. Surv. Bull. 398, 1910. 36 Smith, J. P., Geologic range of Miocene invertebrate fossils of California, Proc. Calif. Acad. Sci., 4th ser., vol. 3, pp. 161-182, 1912. 224 University of California Publications in Geology — [Vou. 10 the approximate equivalent of the San Pablo.’’ The Etchegoin as recognized by Arnold and Anderson was placed in the upper Miocene. The Purisima was believed to be higher than the Etchegoin and of Phocene age. In a short paper by W. A. English*’ on the Fernando near New- hall, Los Angeles County, California, the conclusion was arrived at that the lower Fernando probably does not differ greatly in age from the Etchegoin of Arnold and Anderson. In a recent paper by R. W. Pack and W. A. English** on the region west of the Coalinga district little attempt was made at a faunal study of the Etchegoin. The Jacalitos and Etchegoin were grouped as upper Miocene. According to these writers, ‘‘the Jacalitos and Etchegoin formations are believed to be in the main younger than the true Santa Margarita, although the fauna contained in the lower part of what is mapped as upper Miocene in Waltham Canon shows a close similarity to that of the true Santa Margarita.’’ The Jacalitos and Etchegoin are grouped by Robert Anderson and R. W. Pack*® as upper Miocene, or possibly in part lower Pliocene, and are thought to be of the same age as the San Pablo. By finding remains of land mammals with the marine deposits in the Etchegoin it becomes possible to correlate this group definitely also with distant terrestrial deposits containing only remains of land vertebrates. The mammalian remains have been studied by Professor J. C. Merriam,*® who places both the Etchegoin and Jacalitos of Arnold and Anderson in the Pliocene. The Santa Margarita-San Pablo is placed in the upper Miocene. The study of the San Pablo of middle California by Dr. B. L. Clark apparently shows that this group is of upper Miocene age. The Santa Margarita is considered by him equivalent to the upper part of the San Pablo, while the Etchegoin is recognized as Pliocene. Dr. Clark states that it is his opinion that the Jacalitos is probably vounger than the San Pablo. In a recent publication on the Pliocene of California by Bruce 37 English, W. A., The Fernando Group near Newhall, California, Univ. Calif. Publ. Bull. Dept. Geol., vol. 8, no. 8, 1914. 88 Pack, R. W., and English, W. A., Geology and oil prospects in Waltham, Priest, Bitterwater, and Peachtree valleys, California, U. S. Geol. Surv. Bull. 581D, 1914. 39 Anderson, Robert, and Pack, R. W., Geology and oil resources of the west border of the San Joaquin Valley north of Coalinga, California, U. S. Geol. Surv. Bull. 603, 1915. 40 Merriam, J. C., Tertiary vertebrate faunas of the North Coalinga Region of California, Trans. Am. Philos. Soce., vol. 22, pt. 3, 1915. 1917] Nomland: The Etchegoin Pliocene of Middle California — 225 Martin" the lower Pliocene beds found near Sargent, called San Pablo by Jones, are referred to the same horizon as the Etchegoin. Martin also states that a portion of the Purisima is probably equivalent to a portion of the Etchegoin of Arnold and Anderson. AGE DETERMINATION As will be seen by a comparison of the faunal lists, the lower Etchegoin has a greater percentage of Recent species than the upper division or than the formation as a whole. According to the usual eustom of calculating by the Lyell percentage method, the lower Etchegoin should therefore be placed later in the geologic time-scale than the upper Etchegoin. In this instance we know by undoubted stratigraphic evidence that this is not a fact. We know also that during the deposition of approximately 7000 feet of Pliocene a con- siderable faunal evolution must have occurred. That the percentage method has only a very limited degree of accuracy was shown by Dr. W. H. Dall*® nearly twenty-five years ago in the following statements: There is no doubt that Lyell’s hypothesis has been of great use in settling early Neozoic nomenclature, and has generally hitherto been applied in a manner to which little exception could be taken. But the old conception of the mathe- matical individuality of species has passed away, never to return, and the numerical estimates based upon it are no longer practicable in the absence of any method of determining the personal equation of different palaeontologists in their estimates of what constitutes a species. The classification retaining these names is no longer numerical, but strati- graphic and developmental, and the formations classified under a given name are, for the writer at least, not necessarily synchronous, except where strati- graphically continuous, or synchronic only in a very wide and general sense. It is believed that American geologists are well agreed that the minor sub- divisions of the systems cannot in America at present be subjected to any rigid parallelism with the minor subdivisions of other lands, and that the difficulty of correlation increases with the differences of latitude and distance. Concurring in this opinion, theoretically and practically, no attempt at such correlation has been attempted by the writer within the geological limits assigned to him. It appears, therefore, that the Lyell percentage method ean be apphed only to the larger divisions and only in a very general way. The very fine distinctions which have frequently been made as to the relative age of many of the California Tertiary formations based on 41 Martin, Bruce, The Pliocene of Middle and Northern California, Univ. Calif. Publ. Bull. Dept. Geol., vol. 9, no. 15, 1916. 42 Dall, W. H., Correlation papers, Neocene, U.S. Geol. Surv. Bull. 84, p. 179, 1892. 226 University of California Publications in Geology (Vou. 10 the percentage method are of little value. The finer age determina- tions will probably have to be made by comparing highly specialized forms from the various horizons and by a direct comparison with faunal zones, the position of which has already been found in a section of known stratigraphic sequence. In regard to the Pliocene beds of Florida Dr. Dall** states: In the discussion of these tables, if we adopt the old-fashioned method, it appears that, throwing all doubtful species into the category of extinct forms, we have from the Waccamaw beds 125 out of 180 species still living, or about 70 per cent; while from the Crotan beds we have 80 out of 96 species repre- sented in the recent fauna, or over 83 per cent. By this method the Pliocene character of the beds is obvious, according to the numerical rule. Also for the Miocene of Maryland the same writer** shows that the number of Recent species ranges from 8.5 to 20 per cent. It will thus be seen that the percentage of Recent species in the Etchegoin, 39-- per cent, falls between these two series of figures. The Etchegoin of the Coalinga district rests unconformably on the Santa Margarita, which, as shown by Dr. B. L. Clark,** is probably of the same age as the upper part of the San Pablo. The percentage of Recent species in the San Pablo is 23+. According to Dr. Clark, this would place the San Pablo in the upper Miocene or possibly lower Pliocene. In regard to the mammalian remains found in the Etchegoin Professor J. C. Merriam*® states: ‘‘The time-relations of the Jaca- litos [lower Etchegoin] vertebrates to the faunas of the Great Basin Province are not entirely clear, but the closest relationships seem to be with the lower Phocene.”’ CORRELATION WITH OTHER PLIOCENE FORMATIONS On comparison of the Etchegoin in the region studied by the writer with other Pliocene faunas of California it is found that at no other locality do we find a section that corresponds to the whole Etchegoin studied at Coalinga. The fauna most closely related to the lower Etchegoin is found in the lower Fernando near Newhall, Los Angeles County. Of the sixty 43 Dall, W. H., Tertiary mollusks of Florida, Trans. Wagner Inst. Sci., vol. 3, pt. 2, p. 215, 1892. 44 Dall, W. H., The relations of the Miocene of Maryland to that of other regions and to the Recent fauna, Md. Geol. Surv., Miocene, p. 147, 1904. 45 Clark, B. L., Fauna of the San Pablo Group of Middle California, Univ. Calif. Publ. Bull. Dept. Geol., vol. 8, no. 22, 1915. 46 Merriam, J. C., Tertiary vertebrate faunas of the North Coalinga Region, Trans. Am. Philos. Soc., vol. 22, pt. 3, p. 30, 1915. 1917] Nomland: The Etchegoin Pliocene of Middle California — 227 species listed from that locality, twenty-six are also found in the Etchegoin of Coalinga. Considering the distance by which these localities are separated, a striking resemblance is evident. Among the species strongly suggesting this close relationship may be men- tioned Terebratalia smithi Arnold, Pecten healeyi Arnold, Pecten owent Arnold. With these forms occur also several species unknown except from the lower Fernando near Newhall and from the Etchegoin near Coalinga; these are Chione elsmerensis English, Chione fernan- doensis English, Turris coalingensis Arnold, and Dosinia jacaltosana Arnold. Good specimens of Pecten estrellanus catalinae Arnold, listed by Arnold from the lower Fernando near Newhall, have been obtained by the writer from beds that appear to represent middle Etchegoin at Big Sandy Creek on the west side of the Diablo Range. The fauna most closely related to the upper Etchegoin is undoubt- edly that listed from the lower Pliocene beds at Sargent. Of the thirty-eight species listed from that formation at Sargent, thirty are found in the upper Etchegoin at Coalinga. The species in common include Dendraster gibbsu (Rémond), Pecten etchegoint Anderson and its varieties nuttert Arnold and watts: Arnold. As will be seen by the Etchegoin fauna as summarized in this paper, nearly one-half of the species reported from the Purisima and more than one-half of the species reported from the lower Merced are found in the Etchegoin near Coalinga. The characteristic species common to the Merced, and especially those common to the Purisima, seem to be such as are confined to the middle and upper Etchegoin. It seems probable, however, that the Etchegoin and Merced basins represent different faunal provinces. In the Merced are included several species indicating a closer relationship to the northern forms than the warm water Etchegoin fauna. SUMMARY 1. The accumulation of over 10,000 feet of Pliocene has occurred under shallow marine or terrestrial conditions. 2. In the period in which this accumulation took place the floor of the basin of deposition was several times raised locally above sea-level. After the prevailingly terrestrial conditions had begun marine depo- sition occurred for brief periods. 3. Diastrophic movements of great magnitude occurred in post- Pliocene time in the Coalinga region. 228 University of California Publications in Geology — [Vou. 10 4. The strata above the Santa Margarita and below the Tulare belong to one period of deposition. 5. The Santa Margarita-San Pablo fauna is distinctly different from that of the Etchegoin. 6. As shown by both invertebrates and the vertebrates, the whole Etchegoin is of Pliocene age. 7. An unconformity occurring in the lower portion of what has been mapped as the Etchegoin southeast of Coalinga is probably the line of division of the Etchegoin from the underlying Santa Margarita. 8. An unconformity occurring in the Etchegoin north of Coalinga above the ‘‘Glycimeris zone’’ is probably of only local importance. 9. Four distinct faunal zones have been recognized in the Etche- goin. 10. The lower Etchegoin is most closely related to the lower Fer- nando near Newhall, while the upper Etchegoin is most closely related to the lower part of the Phocene beds at Sargent. DESCRIPTION OF ETCHEGOIN INVERTEBRATE LOCALITIES Out of about two hundred fossil localities in the Etchegoin near Coalinga and in the adjoining regions the following have been selected as showing typically the faunal association of the Etchegoin. All townships and ranges referred to Mount Diablo Base Line and Meridian. 2089. Middle of eastern boundary of NW 44 of NW 4 Sec. 19, T. 19 S, R. 16 E. Mya zone, uppermost Etchegoin. 2091. On west slope of 1100-foot hill near NE corner of NW \ See. 26, T. 19 8, R. 15 E. Vertebrate and invertebrate locality, lowest invertebrate fossiliferous zone. 2093. In creek bed immediately east of 900-foot hill, SE corner of NW % of NW \ See. 13, T. 19 S, R. 15 E. Lowest invertebrate fossiliferous zone, type section of the formation as used by Arnold and Anderson. 2096. Near middle of eastern boundary of SW 4 of SE % Sec. 35, T. 19 8, R. 15 E. In this area the lowest invertebrate fossilferous zone. 2104. Middle of northern boundary of NE % Sec. 12, T. 218, R. 14 E. Upper Etchegoin. 2110. Middle of southern boundary of Sec. 1, T. 218, R. 14 E. Upper middle Etchegoin. 2376. Middle of southern boundary of SE 4 of SW 144 Sec. 6, T. 20 8, R. 16 E. Pecten coalingensis zone. 1917} Nomland: The Etchegoin Pliocene of Middle California 229 2377. Center of NW % of SE \ Sec. 34, T. 19 S, R. 15 E. Lowest invertebrate fossiliferous zone. 2520. Near center of SE 4% of NW % See. 24, T. 21 8, R. 14 E. About 200 yards east of Alcalde-Jacalitos Ranch road. Chione elsmerensis zone. 2523. Center of SE 4 of SE % See. 27, T. 21S, R. 14 E. Short distance west of most southern curve of Alcalde-Jacalitos Ranch road around Curry Mountain, about 15 yards above road. Probably Turritella nova zone. 2526. At junction of Jacalitos Creek and Jasper Creek, near SW corner of Sec. 6, T. 22 8S, R. 15 E. Chione elsmerensis zone. One of typical ‘“Jacalitos’’ localities. 2532. Near top of small ridge on old Coalinga-Stone Canon road, SE corner of NW \ of NW ¥Y See. 21, T. 218, R. 14 E. Chione elsmerensis zone. 2533. Middle of southern boundary of NW 4 of NE 4 Sec. 29, T. 21S, R. 14 E, on north bank of Waltham Creek. Turritella nova zone. 2534. About 100 yards south of B. M. 1699, on old Coalinga-Stone Cafion road, near middle of western boundary of Sec. 31, T. 21 8, R. 14 E. Chione elsmerensis zone. 2535. About 20 yards stratigraphically above 2534. 2616. Near SW corner of NW % of SE \ See. 3, T. 22 8, R. 14 E. Probably Chione elsmerensis zone. 2619. On divide at SE corner of NE 4 of SE \ Sec. 82, T. 218, R. 14 E. Lower middle Etchegoin. 2622. About 20 yards SE of B. M. 1699, Sec. 31, T. 21.5, R. 14 E. Chione els- merensis zone. 2643. South middle part of NE 4 of NW % See. 29, T. 215, R. 14 E. Chione elsmerensis zone. 2649. Near center of NW 4 of SE 4 Sec. 19, T. 21S, R. 14 E. Middle Etchegoin. 2650. At NE corner of SW 4 of SE 4 See. 19, T. 21S, R. 14 E. Middle Etchegoin. 2663. Hast central part of NE 4% of NW 4 Sec. 34, T. 218, R. 14 E. Probably Chione elsmerensis zone. 2664. In saddle of ridge, NE corner of NW \% See. 34, T. 215, R. 14 BE. Turri- tella nova zone. 2669. SW corner of SE 44 of NW % See. 34, T. 218, R. 14 E. Undifferentiated Etchegoin. 2670. On south side of 1600-foot hill near north central part of SW 4% of NW Y% Sec. 34, T. 21, R. 14 E. About middle Etchegoin. 2672. Near center of SE 4% of NW % Sec. 34, T. 21 8, R. 14 E. Chione elsme- rensis zone. 2679. Middle of northern boundary of SE 4 of NE 4 Sec. 7, T. 22.8, R. 15 E. Resistant strata containing Astrodapsis in abundance. Chione elsme- rensis zone. 2680. On ridge, south central part of NW % of NW 14 See. 8, T. 22.8, R. 15 EB. Turritella nova zone. 2684. Near middle of SE 4 of NE 4% See. 12, T. 22 8, R. 14 E. Undifferenti- ated lower Etchegoin. 2693. On ridge extending from 1910-foot hill near NE corner of SW \%4 of NE Y, Sec. 24, T. 218, R. 14 E. Lower middle Etchegoin. 2958. Middle of eastern boundary of NE 4 of NE \4 See. 7, T. 23 8, R. 17 E. Immediately below lowest ‘‘vivianitic’’ sandstone. Turritella nova zone. 2975. 2976. 2977. 2982. 2985. 2986. 2987. 2988. 2991. 3001. 3003. 3004. 3005. 3007. 3010. BOL. 3013. 3016. 3020. University of California Publications in Geology | Vou. 10 2. Near SE corner of NW \ Sec. 7, T. 23 8, R. 17 E. Hard stratum on bank of creek. Chione elsmerensis zone. . NE corner of NW % See. 7, T. 23 8, R. 17 E. Probably Turritella nova zone. . SE corner of NE 14 Sec. 36, T. 22 8, R. 16 E. Immediately north of road. Mya japonica zone. . Near SW corner of NE 144 Sec. 35, T. 22 8, R. 16 E. Upper middle Etchegoin. . Near center of SW \ Sec. 9, T. 23.8, R. 17 E. Probably Turritella nova Zone . At SE corner of See. 8, T. 23 8, R. 17 E. On small branch of creek. Lowest fossiliferous zone in this region. . South central part of SE 4 of SW ¥ See. 8, T. 22 8, R. 16 E. On small creek. Pecten coalingensis zone. About 100 feet above 2974. Pecten coalingensis zone. Near NE corner of NW \ See. 24, T. 22S, R. 15 E, at elevation of about 1500 feet. Chione elsmerensis zone. South central part of SW 14 See. 13, T. 22 8, R. 15 E. Middle Etchegoin. Sec. 8, T. 22 8, R. 16 E. On ridge east of Zapato Creek, about 14 mile SE of Adolph Kreyenhagen’s home. Pecten coalingensis zone. Near SW corner of SE 44 Sec. 20, T. 22S, R. 16 E. Middle Etchegoin. About 50 feet stratigraphically higher than 2985. West central part of Sec. 20, T. 22 8, R. 16 EH. Middle Etchegoin. About 50 yards SE of 2987, about same horizon. Near center of SE 4 See. 17, T. 22.8, R. 16 E. On top of ridge south of road. Pecten coalingensis zone. On bank of creek near center of NW 4 of NW % See. 14, T..20 8S, R. 12 E. Pecten coalingensis zone. On bank of creek near SW corner of Sec. 10, T. 20 8, R. 12 E. Pecten coalengensis zone. West central portion of Sec. 10, T. 208, R. 12 E. Hard stratum on creek bank, short distance above coal. At confluence of two small creeks near center of NE 4 of NE \% See. 9, T. 20 8, R. 12 E. A few hundred feet below coal. Middle Etchegoin. Immediately above pipe line near center of SW 4 of NW ¥ See. 26, T. 208, R. 12 BE. Middle Etchegoin. Near central portion of Sec. 35, T. 205, R. 12 E. Middle Etchegoin. About 600 yards south of 3010. Probably Chione elsmerensis zone. On creek near NE corner of SW 4 of NE \ See. 23, T. 20 S, R. 12 E. Probably float from middle Etchegoin. SE corner of NE 4% of NE \ See. 14, T. 20S, R. 12 E, on bank of creek. Middle Etchegoin. On small branch of creek, near SE corner of Sec. 27, T. 20 S, R. 12 E. Middle Etchegoin. ANTHOZ(| Astrangia coalingensis \ ECHINODER, Astrodapsis jacalitosens Astrodapsis peltoides A1 Astrodapsis, sp. A ....... Dendraster arnoldi Twi Dendraster coalingensis Dendraster gibbsii (Ré Dendraster perrini (W _ Dendraster, sp. A .....-- ‘AxtHor0a araste, aia arnold Gasondia coalingensi® Ba BaacworoDa ebratalia smltht Arnold PELECYPODA eastrensls (Binds) - i (rilianeata Conrad ~ Gardiom corbia (Barty) cordiom quadrigenariom — (Ghana pellaclda Sowerby — hone elsmerensls English Chione fernandoensis English = Crrplomya ealifornica (Conra\ Cepplomsa quadrata Arnold Camingis californica Conrad Cyrens californica Gabb — Diplodonta paris (Conrad) Dosis jncalitosan® ey jmeris coalingensis Arnold aes septentrional (Middendorf) Macoma inquinata (Deshayes) ~ Macowa inquinata aGinis, n- var. Macoma jacalitosana Arnold — Hecoma nasats (Conrad) - Macoma seeta (Conrad) Macoma vanvlceki Arnold Metis alta (Conrad) Modiolus fornicatus Carpenter Modiolus rectus Conrad — Monia macroschisma (Deshayes) Molinia densata Conrad ~ Mya japonica Joy ——— Mytllox coalingensis Arnold Myptilas kewi Nomland —.— Ontren atwoodi Gabb —. Ostrea larida Carpenter Ostrea respertina Conrad Pandora punctata Conrad .. Panops cenerosa Goold — Paphia jacalitosensis Arnold Paphia staleyi (Gabb) staminea (Conrad) ~ tenerrima (Carpenter) ~ coalingensis Arnold egregis, 1. sD. etchegoini Anderson etchegoini nutteri Arnold . Peeten etchegoini wattsi Arnold .... Pecten (Hinnites) giganteus (Gray) - Peeten hastatus hindsii Carpenter Pecten bealeyi Arnold — Pecten owen! Arnold —. Pecten protens, 0. sD. --— Pecten terminus Arnold Periploms argentaria Conrad Petricola carditoides (Conrad) Phacoides annulatus (Reove) Phacoides riebthofeni (Gabb) Panmobia edentula (Gabb) — Prephis lordi (Baird) —... | __Sanguinolsria nattalli Conrad. Saxidomus nuttalli Conrad —. Scbizothaeras nottalli Conrad Semele fausta, n. xp. Siliqaa lucida (Conrad) Solen sicarius Gould Spisula albaria (Conrad) .... Spisola coalingensis (Arnold) Spirals faleata (Gould) Spisala homphilli (Dall) Teina bodegensis Hinds Tivela trigonalis Nomland Thracis formosa, n. sp. Yoldia cooperi Gabb Zirphaes crispata (Linné) .. Gastzoropa Astralium arnoldi Nomland .. Calliostoms coalingensis Arnold ..... Calliostoma etchegoinensis Nomland . Calliostoma kerri Arnold .. Calyptraea filosa (Gab) Cancellaria erassa, n. 6p. cee Cancellaria fernandoenais tribulis, n. var Caneel Cancellaria tritonidea Gabb .. Chrysodomus coalingensis Nomland Chrseodomus imperialis Dall Chrysodomus packardi, n. sp, Chrysodomun portolacnais (Arnold) Te 2663 2976 2077 2082 2086 8005 ypensis Vangie | Colambella (Astyris) richthofent Gabb .. Orepidula adunea Sowerby ... Crepldala princeps Conrad —___ Drillis mercedensix Martin ...... Epitonium varicostata Stearns Ficus nodiferous Gabb .. _— Fissuridea subelliptien Nomland Fissoridea unica, n. sp. ... Littorina mariana Arnold... Margarita johnsoni Arnold .. Marex concinna, n. sp. Murex festivus Hinds ....., ‘Marex perangulatus Nomland ‘Murex tethyn, n. sp. “= ‘Nasa californiana (Conrad) Natiea conyexa Nowland Natlea orbieularis Nomland —___ Natica recluziana Potit —. = Olivella biplicata Sowerby Olivella pedroana (Conrad) ..... Purpura turris Nomland —__ = Torritella vanvlecki Arnold ION enegnsenmees Otuurexpra Balanus concavua Bronn ...... ‘Tamiosoma gregaria Conrad TER TUG ae La i f (! en . blow ae ade . Blowsdé ety j iz yaw) simile 1917] Nomland: The Etchegoin Pliocene of Middle California — 231 DESCRIPTION OF SPECIES ANODONTA NITIDA, n. sp. Plate 9, figure 2 Type specimen no. 11091, Univ. Calif. Coll. Invert. Palae. Shell of moderate size, equivalve, thin, rather compressed, ventral -part of sides of posterior end flattened, with subpentagonal, angular outline. Beaks low, inconspicuous. Anterior region about one-fourth of length of shell; anterior dorsal margin rounded, with shghtly in- creased convexity a short distance in front of beaks; anterior extremity rather sharply angular; posterior extremity slightly truncated ; pos- terior dorsal margin to upper angle of truncation nearly two-thirds of distance from beak to posterior end; from this angle to lower angle of truncation margin is shghtly concave; posterior ventral margin has increased convexity slightly more than one-third of length of shell from posterior end. Surface ornamented by numerous wide concentric ridges. Height, 38 mm.; length, 54 mm. This species may be recognized by compressed form, inconspicuous anteriorly located beaks, angular outline, and flattened posterior ven- tral portion of sides. Occurrence.—At locality 2999, on ridge a little east of middle of southern boundary of see. 12, T. 228, R.17 HE, M. D. B. & M., northern end of Kettleman Hills. At the type locality this species occurs with Goniobasis, sp., in fresh-water horizon at or near the base of the upper Etchegoin. PECTEN EGREGIUS, n. sp. Plate 6, figures 3, 3a, 3b Type specimen no. 11090, Univ. Calif. Coll. Invert. Palae. Shell equilateral, equivalve, thin, rather compressed ; with smooth, regularly rounded base. Dorsal margins long; umbonal angle about 70 degrees. Right valve with about 22-23 moderately strong, rounded ribs; in each interspace there is one small, often invisible, rounded riblet; anterior ear long, arcuate in front, ornamented above byssal notch by about six distinct, radiating ridges and numerous incremental lines; byssal notch well defined; posterior ear very small, sculptured by low radiating ridges and inconspicuous incremental lines. Left valve with about 22 subequal ribs, which are not so prominent as those of the right valve, but with auxiliary riblets more distinet ; anterior ear large, with sculpture consisting of faint incremental lines and about twelve radiating ridges; posterior ear similar to that on the 232 University of California Publications in Geology [Vou. 10 right valve. Dimensions of type, which is a rather small specimen: height, 31 mm.; width, 24 mm.; width of hinge, 13 mm. Occurrence.—At localities 2991, 2975, Pecten coalingensis zone, upper Etchegoin Plocene. PECTEN PROTEUS, n. sp. Plate 6, figures 2, 2a, 2b, 2c Type specimen no. 11089, Univ. Calif. Coll. Invert. Palae. Pecten deserti Conrad. Arnold, Ralph, U. 8S. Geol. Surv. Bull. 396, p. 76, pl. 26, figs. 3, 4, 1909. Pecten deserti Conrad. Arnold, Ralph, and Anderson, Robert, U. 8. Geol. Surv. Bull. 398, pl. 48, figs. 3, 4, 1910. Shell thin, equilateral, equivalve, compressed, with smooth regu- larly convex margins. Dorsal margins slightly concave; apical angle about 95 degrees. Right valve ornamented externally by 21-24 wide, moderately high, rounded ribs; on each side of major ribs is usually a faint auxiliary riblet; interspaces between major ribs less than width of ribs; anterior ear slightly longer than posterior, sculptured by about five low radial ridges and indistinct incremental lines; pos- terior ear ornamented with about seven low, radial ridges and nearly invisible incremental lines. Left valve in general similar to right, but has higher, more strongly rounded, major ribs with narrow inter- spaces; anterior ear with about seven radiating lines. Dimensions of rather small left valve of type: height, 37 mm.; width, 33 mm.; width of hinge lne, 17 mm. Specimens of this species found in the Coalinga region have here- tofore been identified as Pecten deserti Conrad. On comparison of P. deserti from the type locality at Carrizo Mountain, San Diego County, with P. proteus, n. sp., several marked differences may be observed. In P. deserti the ribs are higher, flatter above, with more nearly vertical sides; on the left valve the ribbing continues without interruption from ears over the outer depressed dorsal margins, while in P. proteus, n. sp., the corresponding areas have no ribs. The ears of P. deserti are larger, more strongly curved, and have less depression where ears join dorsal margins of shell: also the dorsal margins show less marked concavity. These instances can be better recognized by seeing the comparative figures shown in this paper. Occurrence.—At localities 2991, 2975, with a large fauna charac- teristic of the Pecten coalingensis zone, upper Etchegoin. 1917] Nomland: The Etchegoin Pliocene of Middle Califorma — 283 MACOMA INQUINATA AFFINIS, n. var. Plate 9, figures 1, la, 1b Type specimen, no. 11092, Univ. Calif. Coll. Invert. Palae. Shell large, equivalve, short, trapezoidal, with rather long liga- mental groove. Sides moderately convex, slightly excavated a little below anterior dorsal margin, giving a flange-like appearance, with depressed area on both valves extending from umbones to posterior dorsal margin. Beaks low, adjacent, a little anterior to middle. Anterior margin evenly rounded, with increased convexity at anterior extremity; posterior dorsal margin arcuate, with greater curvature behind ligamental groove; posterior ventral margin concave where intersected by depression extending from beak, on most specimens base more strongly curved a little posterior to middle. Surface covered by numerous, unequal, concentric lines. Dimensions: height, 52 mm. ; length, 64 mm. This species may be distinguished from the typical Macoma inqui- nata (Deshayes) by its larger size, the flange immediately anterior to the beaks, depressed area extending from umbones to posterior ventral margin, rather long ligamental groove, and increased convexity near middle of base. Occurrence.—Loeality 2965, Mya japonica zone, uppermost Etche- goin. SEMELE FAUSTA, n. sp. Plate 9, figures 3, 3a, 3b Type specimen no. 11102, Univ. Calif. Coll. Invert. Palae. Shell small, inequilateral, with moderately convex valves and low beaks. Posterior end much shorter than anterior; anterior dorsal margin straight, with evenly rounded anterior end; posterior dorsal margin slightly convex, with posterior end truncated inwards. Sur- face sculptured by numerous, about equidistant, low, concentric lines; with a nearly obsolete fold extending from the beaks to the posterior end. Resilifer weak, narrow; ligamental groove almost obsolete. Right valve with long, rather low laterals; anterior cardinal indistinct, posterior cardinal low and slender; left valve with feeble laterals and indistinct, thin cardinals. Dimensions: length, 35 mm.; height, 30 mm. This form is of the same general type as Semele rubropicta Dall, from which it may be distinguished by its having a greater length in proportion to the width, the anterior portion being longer, the fold 234 University of California Publications in Geology [Vou. 10 more nearly obsolete, and by the long, straight, anterior dorsal margin. The hinge also differs in having the weak, narrow resilifer and long, narrow laterals, this being especially true of the anterior teeth. Occurrence.—At locality 2991, upper Etchegoin, on Zapato’ Creek, Fresno County; at the type locality this species occurs with Thracia formosa, n. sp., Fissuridea unica, n. sp., Tegula (Chlorostoma) pulcella, n. sp., and the associated fauna. THRACIA FORMOSA, n. sp. Plate 9, figures 4, 4a Type specimen no. 11103, Univ. Calif. Coll. Invert. Palae. Shell small, inequilateral, thin, moderately compressed. Beaks low, about three-fifths length of shell from anterior end. Posterior dorsal margin slightly convex; posterior end truneated. Junction of anterior dorsal and ventral margins marked by slight increase in con- vexity. Ventral margin evenly arcuate. Surface ornamented by dis- tinct, uniform, rounded, concentric ridges; with a well developed, broad suleation extending from the beak to the posterior extremity. Hinge weak; right valve with small, rather thick tooth projecting at angle of nearly 45 degrees to plane of shell. Dimensions: height, 27 mm.; width, 19 mm. Occurrence.—At loeality 2991, with a large fauna characteristic of the upper Etchegoin. FISSURIDEA UNICA, n. sp. Plate 11, figures 3, 3a, 3b Type specimen no. 11100, Univ. Calif. Coll. Invert. Palae. Shell subovate, conical, elevated, straight to shghtly convex sides, with apex a little anterior. Ornamented by numerous prominent, rounded, rather thin, radiating ridges with narrow interspaces. In- cremental lines unequal, often more prominent than the radiating ridges. Apical orifice oblong, anterior to the apex, bounded inside by a posteriorly truneated callus. Dimensions of type, which is a rather small specimen: height, 14 mm.; maximum diameter, 25 mm.; mini- mum diameter, 19 mm. | This species can readily be recognized by its height, ovate base, and radial ribbing with narrow interspaces. Occurrence.—In the upper Etchegoin, with a large fauna of the Pecten coalingensis zone at locality 2991. . = 1917] Nomland: The Etchegoin Pliocene of Middle California 20 TEGULA (CHLOROSTOMA) PULCELLA, n. sp. Plate 12, figures 3, 3a Type specimen no. 11101, Univ. Calif. Coll. Invert. Palae. Shell conical, thin, with about six whorls; suture distinct, ap- pressed. Sides of whorls flat, giving an almost uniform slope from apex to base. Surface striated by faint, oblique, incremental lines and numerous low, rounded, axial riblets; on the sides of the whorls near the base are about three fine spiral threads. Base of body-whorl flattish, with sharp angle at periphery; ornamented by incremental lines and two or three nearly obsolete spirals around umbilical area. Aperture subquadrate, with thin outer lip; inner Lp with two small tubercles, of which the lower is almost invisible. Umbilicus open; outer edge of umbilical area limited by a distinct, sharp ridge. Height, 23 mm.; diameter of slightly deformed type, 26 mm. This species is easily recognized by its flat sides, conical form, and low axial ornamentation. Occurrence.—At locality 2991, with a large fauna of the Pecten coalingensis zone, upper Etchegoin. CHRYSODOMUS PACKARDI, n. sp. Plate 12, figures 4, 4a, 4b Type specimen no. 11096, Univ. Calif. Coll. Invert. Palae. Shell thick, has about four or five rapidly increasing whorls, with distinct, appressed suture. Whorls slightly convex, tabulate, almost channeled above. Surface of whorls ornamented by coarse, square, spiral ribs, between which are fine thread-like interealaries and narrow interspaces; on body-whorl and continuing nearly to lower end of canal there are about nine and on the whorls of spire three of these major spirals. Crossing the whorls, and especially evident on spire, are numerous longitudinal ribs ; on body-whor! of some specimens these ribs become nearly obsolete; where spirals cross the axial ribs a retic- ulate appearance is produced. Aperture rectangular, forming a short, wide canal; with thin, sharp, outer lip; inner lip inerusted, smooth. Dimensions of type: diameter, 17 mm.; height unknown. Occurrence.—At localities 2958, 2985, middle Etchegoin. At the type locality near middle of western boundary of NW 14 of NW 4 sec. 8, T. 23.8, R. 17 E, M. D. B. & M., this species occurs with the following species: Arca trilineata Conrad, Calliostoma, ef. kerri Ar- 236 University of California Publications in Geology | Vou. 10 nold, Calyptraea filosa (Gabb), Dendraster, sp., Macoma, ef. inquinata (Deshayes), Nassa californiana (Conrad), Ostrea atwoodi Gabb, Paphia staminea (Carpenter), Thais kettlemansis Arnold, Trophon, sp., Turritella, ef. nova Nomland. MUREX (OCINEBRA) CONCINNA, n. sp. Plate 12, figures 6, 6a Type specimen no, 11093, Univ. Calif. Coll. Invert. Palae. Shell small, subfusiform, with rather low spire. Whorls four or more, increasing rapidly in size. Body-whorl with distinct angles at shoulder and base, giving the sides a flattened appearance. Each whorl with about nine wide, prominent, axial ribs; on body-whorl these extend from suture down to about middle of canal. The spiral orna- mentation on the body-whorl consists of about eight and on the spire two, high, rounded cords which become fainter on canal ; between these, especially on upper part, are fine thread-like interealaries; where the spirals intersect the axial ribs a decidedly nodose appearance is pro- duced. Aperture oblong-elliptical; outer lp thickened, terminating in a long, narrow, recurved canal; inner lip slightly inerusted ; colu- mella faintly marked by spiral sculpture. Dimensions: height, 25 mm. ; maximum diameter, about 13 mm. Occurrence.—At localities 2643, 2985, middle Etchegoin. MUREX (OCINEBRA) TETHYS, n. sp. Plate 12, figures 2, 2a, 2b Type specimen no. 11099, Univ. Calif. Coll. Invert. Palae. Shell small, heavy; whorls four or five; suture distinct, slightly channeled; apex acute; body-whorl large and ventricose. Whorls sculptured by prominent, coarse spiral cords and low, often almost invisible, interealaries; the body-whorl has about seven and the spire two of the major cords; these are crossed by eight high, angular, longi- tudinal ribs which disappear on lower part of body-whorl; where these cross the spirals the shell becomes slightly nodose, this being especially evident on upper part of whorls, where a rather sharp shoulder is produced. Aperture wide, elliptical, with thick outer lip; inner lip apparently smooth, incrusted; canal short, slightly curved. Dimen- sions of type: height, 21 mm.; diameter, 15 mm. Apparently this form most closely resembles Ocinebra lurida, var. cerritensis Arnold, from which it may be distinguished by its higher 1917] Nomland: The Etchegoin Pliocene of Middle Califorma — 237 and more acute spire, the presence of small spiral intercalaries, and the sharper angle at shoulder of whorls. Occurrence.—At localities 2986, 2985, 2988, 2643; middle Etche- goin. TROPHON BELCHERI AVITUM, n. var. Plate 11, figure 5 Type specimen no. 11094, Univ. Calif. Coll. Invert. Palae. Shell large, heavy, with five or more whorls; spire moderately elevated ; suture appressed. Whorls angulate at shoulder, with promi- nent angle at lower part of body-whorl; immediately below this is a deep groove which varies considerably in size in different specimens and in front of which the lower part of body-whorl protrudes. Whorls and canal ornamented by about eleven raised axial folds or varices which at the shoulder become sharp spines, also at lower angle of body-whorl where intersected by varices the shell usually becomes nodose. Outer lip thin, eanal slightly recurved. Height of type, 66 mm.; diameter of body-whorl, 60 mm. This species differs from Trophon belchert Hinds by shorter and stouter nodes at shoulder, rather prominent nodes near base of body- whorl, shorter columella, and lower spire than most specimens of T. belcherr. From T. magister Nomland it differs in having a larger number of varices, in being more spinose at shoulder, and by more evident development of nodes on lower part of body-whorl. An interesting problem in evolution could probably be solved by a study of the large Trophons having the characteristic groove 1mme- diately below the body-whorl. In the lower Miocene this type first appears as 7’. gabbianum Anderson; in the upper Miocene it takes the form of 7. carisaensis Anderson; in the Pliocene we find 7. magister Nomland, while the Recent form is 7’. belcheri Hinds. Occurrence.—At locality 2988, middle Etchegoin. CANCELLARIA CRASSA, n. sp. Plate 12, figures 7, 7a Type specimen no. 11098, Univ. Calif. Coll. Invert. Palae. Shell slender, solid, with about five whorls; suture distinet, im- pressed. Whorls sharply angulated a little less than one-third of the distance below suture, somewhat tabulate above; near the base of the body-whorl is another distinet angle, giving the periphery of whorls 238 University of California Publications in Geology — [Vou. 10 a flattened appearance. Axially seulptured by eleven prominent ribs which become less marked on the tabulate portion above, on the body- whorl these extend only to lower peripheral angle. Spiral sculpture on the body-whorl consists of seven and on the spire five strongly elevated cords. Outer lp of type defective. Aperture narrow, with long twisted canal. Inner lip slightly inerusted, pillar long and slender, with two thin, sharp plaits on the lower part. Height, about 41 mm.; diameter, 20 mm. Occurrence.—At locality 2533, near middle of southern boundary of NW ¥, of NE ¥, sec. 29, T. 21S, R. 14 E, M. D. B. & M., on north bank of Waltham Creek. At the type locality this form oceurs with the following characteristic Etchegoin species: Macoma vanvlecki Arnold, Pecten terminus Arnold, Pecten owent Arnold, Phacoides annulatus (Reeve), Bathytoma tryoniana (Gabb), Ficus nodiferous Gabb, Turris coalingensis (Arnold), Thais kettlemanensis Arnold, Turritella nova Nomland. CANCELLARIA FERNANDOENSIS TRIBULIS, n. var. Plate 12, figures 1, la Type specimen no. 11095, Univ. Calif. Coll. Invert. Palae. Shell broadly fusiform, spire high, with about four whorls; body- whorl large; suture distinct, almost channeled. Whorls with sharp angle immediately below suture, giving a tabulate appearance to the upper part; sculptured with about sixteen prominent axial ribs, which on the body-whorl become less distinct above the shoulder and are almost obsolete on the canal. Spiral ornamentation on the body-whorl consisting of twenty-two, and on the whorls of the spire about nine, nearly equal cords with narrow interspaces, which on crossing the axial ribs form nodes. Aperture ovate, forming a short, slightly twisted canal. Pillar nearly straight, covered by a thin coat of callus; with two broad, low plaits with wide interspaces. Dimensions: height, 34 mm.; diameter, 19 mm. This variety has fewer axial ribs, shoulder is higher up on the whorls, upper surface of whorls more distinctly tabulate, and whorls enlarge more rapidly than the typical form. Occurrence.—At locality 2964, on low hills near divide between Big Tar Creek and Garza Creek, near center of NE 144, of NW 14, see. 7, T. 238, R.17 E, M. D. B. & M., middle Etchegoin Pliocene. At the type locality this species oceurs with a fauna including the following 1917} Nomland: The Etchegoin Pliocene of Middle California — 289 species: Arca trilineata Conrad, Chrysodomus portolaensis (Arnold), Dendraster gibbsii (Rémond), Olivella biplicata Sowerby, Paphia staminea (Carpenter), Pecten, ef. healeys Arnold, Pecten terminus Arnold. PECTEN ETCHEGOINI Anderson Plate 7, figures 1 to 5 Pecten etchegoini Anderson, Proe. Calif. Acad. Sci., vol. 2, p. 198, pl. 18, figs. 92-93, 1905. Pecten wattsi, var. morani Arnold, U. 8. Geol. Surv. Prof. Paper 47, pp. 121-122, pl. 10, figs. 3-6, 1906. Pecten wattsi Arnold, var. etchegoini “Anderson, U. 8. Geol. Surv. Bull. 396, p. 77, 1909. On obtaining a large number of specimens from the type localities of Pecten etchegoint Anderson, P. nuttert Arnold, and P. wattsi Arnold a difficulty was at once experienced in attempting a separation of these forms. By closer study it was found that the prominence of the ribs of P. etchegoini varies greatly. Also the nodose constrictions characteristic of P. wattsi vary much in prominence. It became evi- dent that series could be found for both valves showing a gradation of P. nuttert and P. wattst into P. etchegoin. Figures are given in the present paper showing gradational series. P. nutteri Arnold and P. wattst Arnold are therefore here used as variations of P. etchegoini Anderson. SERPULA (?), sp. Figure 2 , On the south bank of Garza Creek, in the Coalinga district, is exposed a bed composed almost exclusively of tubules believed to represent the genus Serpula. The tubules are about 1.5 mm. in diameter and are closely packed together, forming an almost solid mass. 240 University of Californa Publications in Geology — [Vou. 10 CANCELLARIA RAPA, n. sp. Plate 11, figures 1, la Type specimen no. 11097, Univ. Calif. Coll. Invert. Palae. Shell thick, ventricose, with about five or six rapidly enlarging, regularly convex whorls, apex rather blunt. Suture marked by a dis- tinct line, slightly appressed. Sculpture consisting of spiral ridges crossed by low axial riblets. Spiral sculpture on the body-whorl marked by about eighteen nearly square major ribs; between most of these are less prominent interecalaries with interspaces narrower than the latter. Axial riblets not regularly spaced, nearly obsolete, be- coming entirely so on lower half of body-whorl. Aperture semilunar, outer lip broken, forming a short canal at base. Pillar thinly inerusted and with four plaits, of which the middle and lowest are less prominent. Height of type, 53 mm.; diameter, 29 mm. Occurrence.—The type in the University of California collections, obtained by L. D. O'Neal, is labeled as having come from the Phocene(?) near Coalinga, Fresno County, California. cy ‘ \ EXPLANATION OF PLATE 6 All figures approximately natural size Fig. 1. Pecten deserti Conrad. Right valve; from the type locality at Car- rizo Creek, San Diego County; Carrizo formation, Pliocene. Fig. la. Pecten deserti Conrad. Left valve; from the type locality. Fig. 1b. Pecten deserti Conrad. Profile view from the rear of the same specimen as figure la; showing on the left valve ribbing continuing from body over ears without interruption. Fig. 2. Pecten proteus, n. sp. Left valve of type from locality 2991; Univ. Calif. 11089; Pecten coalingensis zone, upper Etchegoin. Fig. 2a. Pecten proteus, n. sp. Right valve; from locality 2991. Fig. 2b. Pecten proteus, n. sp. Right valve; from locality 2991. Fig. 2c. Pecten proteus, n. sp. Profile view from rear of same specimen as figure 2; showing unribbed area immediately above ear. Fig. 3. Pecten egregius, n. sp. Left valve; from locality 2975; Pecten co- alingensis zone. Fig. 3a. Pecten egregius, n. sp. Right valve of type; from locality 2991, no. 11090, Pecten coalingensis zone, upper Etchegoin. Fig. 3b. Pecten egregius, n. sp. Profile view from rear of same specimen as figure 3a. Fig. 4. Pecten terminus Arnold. Right valve; from locality 2523. This species was described as a variety of Pecten estrellanus Conrad by Arnold. [242] WINIV CALIF, PUBL. BULL. DEPT.. GEOL. [NOMLAND] VOL 10, PL. 6 EXPLANATION OF PLATE 7 All figures natural size, left valve. Figures 1 to 4 from locality 2975. Figures showing gradation of Pecten wattst Arnold and Pecten nutteri Arnold into Pecten etchegoini Anderson. Fig. 1. Pecten etchegoint Anderson. From the type locality of the species, Zapato Creek, Fresno County. Fig. la. Pecten etchegoini Anderson. Fig. 1b. Pecten etchegoini Anderson, or P. etchegowmi, var. wattsi Arnold. Fig. le. Pecten etchegoini wattsi Arnold. From the type locality of the variety, Zapato Creek, Fresno County. Fig. 2. Pecten etchegoini wattsi Arnold. Fig. 3. Pecten etchegoini watts: Arnold, or var. nutteri Arnold. Fig. 4. Pecten etchegoini nutteri Arnold. From the locality from which Arnold’s material was obtained, Zapato Creek, Fresno County. Fig. 5. Pecten etchegoini nutteri Arnold. From locality 2982. [244] Reaw 10, [NOMLAND] VOL. DEP GEO UNIV, CALIF, PUBL. BULL. EXPLANATION OF PLATE 8 All figures approximately natural size Fig. 1. Cryptomya quadrata Arnold. Right valve; from locality 3005, Priest Valley, Monterey County. Fig. la. Cryptomya quadrata Arnold. Left valve; from same locality as figure 1, Fig. 2. Pecten etchegoini Anderson. Right valve; from locality 3004, Priest Valley, Monterey County. Fig. 2a. Pecten etchegoini Anderson, or P. etehegoini nutteri Arnold. Right valve of an intermediate form; from locality 3004. Fig. 2b. Pecten etchegoini nutteri Arnold. Right valve; from locality 3004. Fig. 8. Macoma vanvlecki Arnold. Right valve; from locality 2526, Jaca- litos Creek, Fresno County. Fig. 3a. Macoma vanvlecki Arnold. Left valve; from locality 2526. [246] aes 10, [NOMLAND] VOL. UINIV. 2CALIF. PUBL, BULL. DEPT. GEOL. 2 Fae Sean e Se x 4 EXPLANATION OF PLATE 9 All figures approximately natural size Fig. 1. Macoma inquinata affinis, n. var. Left valve; no. 11092; from locality 2965, Garza Creek, Kings County, uppermost Etchegoin. Fig. la. Macoma inquinata affinis, n. var. Right valve of same specimen as figure 1. Pig. 1b. Macoma inquinata affinis, n. var. Profile view of valves shown in figures 1 and la. Fig. 2. Anodonta nitida, n. sp. Left valve; a fresh-water species from locality 2999, no. 11091, Kettleman Hills, Kings County. Fig. 3. Semele fausta,n. sp. Right valve; from locality 2991, Zapato Creek, Fresno County; no. 11102; Pecten coalingensis zone, upper Etchegoin. Fig. 3a. Semele fausta, un. sp. Hinge of left valve; from locality 2991. Fig. 3b. Semele fausta, n. sp. Hinge view of same specimen as figure 3. Fig. 4. Thracia formosa, nu. sp. Left valve; from locality 2991, Zapato Creek, Fresno County; no. 11108; Pecten coalingensis zone, upper Etchegoin. Fig. 4a. Thracia formosa, n. sp. View of hinge of same specimen as figure 4. [248] UNIV: CALIF... PUBL. BULL. DEPT. GEOL. [NOMLAND] VOL. 10, PL. 9 EXPLANATION OF PLATE 10 Figures approximately of natural size Fig. 1. Dosinia jacalitosana Arnold. Exterior of right valve; from locality 3012, Priest Valley, Monterey County; lower Etchegoin. Fig. la. Dosinia jacalitosana Arnold. View of hinge of right valve; from locality 3012. [250] ‘. UNIV. CALIF. PUBL. BULL. DEPT. GEOL. [NOMLAND] VOL. 10, PL. 10 _— = VF s7 —— _ “a: a —— — oe —r-lC(<(C WCU = a EXPLANATION OF PLATE 11 All figures approximately natural size Fig. 1. Cancellaria rapa, n. sp. Mouth view; no. 11097; Etchegoin Pliocene. Fig. la. Cancellaria rapa, n. sp. Opposite view of same specimen as figure 1. Fig. 2. ELpitoniwm varicostata Stearns. Mouth view; from locality 2975, Zapato Creek, Fresno County; Pecten coalingensis zone, upper Etchegoin. Fig. 8. Pissuridea unica, nu. sp. Top view of type; no. 11100; from locality 2991, Zapato Creek, Fresno County; Pecten coalingensis zone, upper Etchegoin. Fig. 3a. Fissuridea unica, n. sp. Side view of same specimen as figure 3. Fig. 3b. Fissuridea unica, n. sp. Side view of a specimen of medium size; from locality 2991. Fig. 4. Purpura turris Nomland. Mouth view; from locality 2680; occurs in both lower and upper Etchegoin. Fig. 4a. Purpura turris Nomlarnd. Opposite view of same specimen as figure 4. Fig. 5. Trophon belcheri avitum, n. var. View of back; no. 11094; from locality 2988, Zapato Creek, Fresno County; middle Etchegoin. UNIV: CALIF. PUBL. BULL. DEPT, “GEOL. [NOMLAND] VOL. 10, PL. II EXPLANATION OF PLATE 12 All figures approximately natural size Fig. 1. Cancellaria fernandoensis tribulis, n. var. Mouth view; no. 11095; locality 2964, Garza Creek, Kings County; Turritella nova zone. Fig. la. Canecellaria fernandoensis tribulis, un. vary. Same specimen as figure 1 viewed from opposite side. Fig. 2. Murex tethys, n. sp. Back view of type; no. 11099; from locality 2986, Zapato Creek, Fresno County, middle Etchegoin. Fig. 2a. Murex tethys, n. sp. View of back of a small specimen; from locality 2643, Fig. 2b. Murex tethys, n. sp. Mouth view of same specimen as figure 2. Fig. 3. Vegula (Chlorostoma) pulcella, n. sp. From locality 2991, Zapato Creek, Fresno County; no. 11101; Pecten coalingensis zone, upper Etchegoin. Fig. 3a. Tegula (Chlorostoma) pulcella, n. sp. Same specimen as figure 3; view of distorted and broken base. Fig. 4. Chrysodomus packardi, n. sp. View of back of type; no. 11096; from locality 2958, Big Tar Creek, Kings County; middle Etchegoin. Fig. 4a. Chrysodomus packardi, n. sp. Mouth view of distorted specimen from locality 2985. Fig. 4b. Chrysodomus packardi, n. sp. View of back of specimen from locality 2958. Fig. 5. Turritella vanvlecki Arnold. From locality 2577, the type locality of the species. Fig. 6. Murex concinna, n. sp. Mouth view; no. 11093; from locality 2643, lower Etchegoin. Fig. 6a. Murex concinna, n. sp. View of back of same specimen as figure 6. Fig. 7. Cancellaria crassa, n. sp. Mouth view; no. 11098; from locality 2533, Waltham Creek, Fresno County; Turritella nova zone, middle Etchegoin. Fig. 7a. Cancellaria crassa, n. sp. Back view of same specimen as figure 7. [254] od UNIV CALIF, PUBL: BULL; DEPT. GEOL. [NOMLAND] VOL. 10, PL. 12 ‘CALIFORNIA PUBLI ULL OF THE DEPARTMENT OF fe. GEOLOGY |.” 4 pp. 255-266, plate 13 ~ Issued April 14, 1917 G FORMATION IN THE WHITE BLUFFS _ OF THE COLUMBIA RIVER BY JOHN C. MERRIAM anp JOHN P. BUWALDA UNIVERSITY OF CALIFORNIA PRESS BERKELEY Nore.—The University of California Publications are s ofterer in e eations of learned societies and institutions, universities and libraries. all the publications of the University will be sent upon request. For sa publications and other information, address the Manager of the University Pi California, U. S. A. All matter sent in exchange should be addressed a a Department, University Library, Berkeley, California, U. S. A. Otto HaRRASSOWITZ R. FRIEDLAENDER & LEIPZIeé ; : BERLIN 3 Agent for the series in American Arch- Agent for the series in Ami aeology and Ethnology, Classical Philology, aeology and Ethnology, Agricultv Heonomics, Education, History, Modern Botany, Geology, Mathematics, Philology, Philosophy, Psychology. Physiology, Zoology, and Memoir Geology.—AnpDREwW C, LAwson and JoHN-C. Murriam, Editors. Price, volumes 1-7, volumes 8 and following, $5.00. ay Cited as Univ. Calif. Publ. Bull. Dept. Geol. Volume 1, 1893-1896, 435 pp., with 18 plates, price .......-.---..---s-:csseccse-0 Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price haste Volume 3, 1902-1904, 482 pp., with 51 plates, price posttosasbenuecuta loves cuntite: seen Volume 4, 1905-1906, 478 pp., with 51 plates, price Volume 5, 1906-1910, 458 pp., with 42 plates, price A list of titles in volumes 1 to 5 will be sent upon request. VOLUME 6. . The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller... eee . Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern — Nevada, by John C. Merriam. . Part I.—Geologie History..............--:c-esee-ssssess-cseeastes ‘ 50 The Geology of the Sargent Oil Field, by William FP. Jones -200.0....:-cceceececeseceececeeseeee “m2 Additions to the Avifauna of the Pleistocene Deposits at Fossil Lake, Ortgen by Love, Holmes Miller y.5.2c. co 2p.c---cssnsnsesbrccqnnmnecer een e epee eee Eanaeeeee Aen eerie eae 5. The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Reid 6. Note on a Gigantie Bear from the Pleistocene of Rancho La Brea, by John C. 7 Pe poe Merriam. ot . A Collection of Mammalian Remains from Tertiary Beds on the Mohave Desert, te, by John C. Merriam. * Nos. 6 and <7-IN, ONC COVED <2250-.22osthcccne ox bape -dacnapunbeere ns toch eta e oneencni =e ee eae 8, The Stratigraphic and Faunal Relations of the Martinez Formation to the ‘Chico and Tejon North of Mount Diablo, by Roy EH. Dickerson .........2...--.csscsssssecnreeenoens 9. Neocolemanite, a Variety of Colemanite, and Howlite from fang, Los Angeles County, California, by Arthur S, Hake no. i occc. eke See ncn tae ee 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. Taylor... BAe 11. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern Nevada, by John C. Merriam. Part Il.—Vertebrate Paunas ...........-.e-ccesceseeco-e-e Be 12. A Series of Eagle Tarsi from the Pleistccene of Rancho La Brea, by Loye Holmes Maer on. nec cece cence ceeennsane Hee a peta pan a son Onen dence one bk ecg carn ea a ee rr ali 13. Notes on the Relationships of the Marine Saurian Fauna Deseribed from the Triassic = of Spitzbergen by Wiman, by John C. Merriam. : 14. Notes on the Dentition of Omphalosaurus, by John C, Merriam and Harold C. Bryant, — Nos:13 and 14 in one cover. 2.5.2.5 locke ci ose sense ae pee a 15. Notes on the Later Cenozoic History of the Mohave Desert Region in Southeastern California, by Charles Laurence Baker: -1.2:.:-scessssutnsssse:soscbpedeecanecns lars eneeote er 16. Avifauna of the Pleistocene Cave Deposits of California, by Loye Holmes Miller poss 17. A Fossil Beaver from the Kettleman Hills, California, by Louise Kellogg ............ ne 18. Notes on the Genus Desmostylus of Marsh, by John C. Merriam ...........20-0:---0-0- abe 19. The Elastic-Rebound Theory of Earthquakes, by Harry Fielding Reid —..- aon VOLUME 7. . The Minerals of Tonopah, Nevada, by Arthur S.. Halle sscccccescecsnceenssersstnrsseese re . Pseudostratification in Santa Barbara County, California, by George Davis ‘Tonia ) 2: nan oe ee eR RO Re HR SABE Niece case tarti: ser nperenntoeccatnc nn . Recent Discoveries of Carnivora in the Eletevovens of Rancho La Brea, by BAU GS eT 0 ee en ee eer ec a ce een eer oe choca cea E Sn socoaeeeee seen aoe . The Neocene Section at Kirker Pass on the N. orth Side of Mount Diablo, by Br t Wy. Gd ars oi or ond we Soha nab bates soot ennncdeaatesaucceade eben ensenetaat sedan ceeie aces ae Z Contributions to Avian Palaeontology from the Pacifie Coast of North Auerion, Loye ee Miller. 2. cnc 2p. sioal gasasnabe te ceeca eects cnt ee ea oO f «w Pe UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 15, pp. 255-266, plate 13 Issued April 14, 1917. y \ AGH OF STRATA REFERRED TO THE ELLENS- BURG FORMATION, Ww THE WHITE BLUFFS OF THE COLUMBIA RIVER BY JOHN C. MERRIAM anp JOHN P. BUWALDA CONTENTS PAGE SPorecaTs OCH CSCO Ite oo seess encase ere Nee ceo Lot coach vac gctcecadounven dete redertncnalincperecces 255 TE secooreuess eran ei Meare h nag R 256 TOSI TEENS — cccconosceec beet cc peel i Se Be i ee a So ESP 257 (QeCODO GY cssccrctiter ee U2 eM Ao a ee 260 SPUN UOTE CHSC CLIO My teen sett acute nea laa Sic. J wees seas Ne sags beeen eben ssteds ness cecebecsacueteces 260 hy Slo omaphiy, amd StVUCtUre) -..22. 28sec ceeet ecco ceteeteet ened Sg 261 BAVT@ LS aE. CUS KORE a A ER 263 BSCE comme ete le tia i, SEL Ee ae A BE PEE 263 ielation’ to’ the Hllensburg formation: -.2.. 222.2220. ieee cee eeee cena 264 INTRODUCTION As a part of a programme of correlation studies on the Tertiary in the northern part of the Great Basin, the writers visited important localities of the Ellensburg formation of south-central Washington in June, 1916, in the hope of adding to the scanty representation of vertebrate remains known from these beds. A small collection was secured in the type area of the Ellensburg formation near North Yakima. A somewhat larger quantity of fragmentary material was collected in the great section of sediments appearing in the White Bluffs of the Columbia River in the vicinity of Hanford and Ringold, generally recognized as one of the largest of the typical Ellensburg exposures. In the typical Ellensburg area near North Yakima remains of an equid or horse type were found representing the genus Hipparion, 256 University of California Publications in Geology — [Vou. 10 a group especially well represented in the earlier Pleistocene of western North America. From the White Bluffs localities the only determinable specimens representing the horse family belong to an advanced or specialized species of the genus Equus. In the widely known North American occurrences of Hquus there is as yet no reported discovery of a species of such an advanced type in beds earher than Pleistocene. It is quite certain that the evolution stages of the horses rep- resented by the Ellensburg and White Bluffs specimens belong to widely different periods, of which the White Bluffs stage is the later. The Ellensburg formation is evidently Miocene to early Plio- cene in age; the White Bluffs exposures represent a distinct and considerably later stage in the history of sedimentation in the eastern Washington region. It is the purpose of the following paper to give a brief statement concerning the physiographie and geologic features and the fauna of the White Bluffs exposures, which are here described as the Ringold formation. , Owing to brevity of the time spent in the Ringold area by the writers, data concerning structure of the formation, extent of the area occupied, and stratigraphic relations to the Ellensburg formation must be considered incomplete. PREVIOUS KNOWLEDGE The White Bluffs section was considered by I. C. Russell? ‘‘the most typical section of the John Day beds to be seen in Washington.’’ As the name John Day was used by Russell with reference to the formation now known as the Ellensburg, it is to be presumed that he considered the White Bluffs approximately contemporaneous with the Ellensburg. The exposures were stated by Russell to range up to 500 feet in height, and to be composed of approximately horizontal or only slightly tilted strata. The beds were reported to consist of fine sands, clays, and strata of voleanie ash. A section taken at the southern end of the cliffs measured 496 feet in thickness. Russell ? reported that fossil bones of large animals had been found in the White Bluffs beds, but that their significance was not known. The exposures were considered favorable ground for collect- ing vertebrate remains. Reference was made to deposits presumed 1U. 8. Geol. Surv. Bul. no. 108, p. 97, 1893. 2 Tbid., p. 98. 1917] Merriam-Buwalda: White Bluffs of the Columbia 257 to be Pleistocene in the region occupied by the White Bluffs sedi- ments, and the possibility noted of confusing Pleistocene and White Bluffs beds. Russell mentioned a locality at the southern end of the White Bluffs exposures, about fifteen miles above Pasco, where a number of large fossil bones, assumed to have been derived from the White Bluffs beds, were found in a river terrace banked against a cliff formed of horizontal White Bluffs strata. He stated that no molluscan shells were found in the sediments, and suggested the possibility that immense quantities of voleanie dust falling into the water may have made it unfavorable for animal life. In 1903 George Otis Smith* referred to the White Bluffs exposures described by Russell, and called attention to evidence indicating that while in the Yakima region the Ellensburg formation is of fluviatile origin, farther east along the Columbia the formation is of lacustrine character. Calkins* discussed the White Bluffs in 1905, and gave from the upper end of the cliffs a section 225 feet in thickness, consisting of sands and clays with some ashy material. Other writers were followed in correlating the White Bluffs exposures with the Ellens- burg, but Calkins noted that ‘‘the general character of this section offers some points of contrast with the typical section measured in the Ellensburg Quadrangle.’’ The materials included in the White Bluffs exposures were shown to be fine and less commonly cross-bedded than in the typical Ellensburg, and tuffaceous material was stated to be less abundant. The suggestion was made that a part of the White Bluffs beds may be of lacustrine origin, but that certain of the sandy layers were probably laid down in rivers. Calkins found no fossils in the White Bluffs exposures, but noted the reported occurrence of shells and bones in the bluffs near Pasco. FAUNAS In examining the White Bluffs in June, 1916, the authors collected mammalian material from exposures about midway between the base and the summit of the bluffs on the east side of the Columbia three to four miles below Hanford (loc. 3031). Later in the summer a small collection was secured one or two miles north of Ringold School (loe. 2757) a few miles south of the first locality. 3U. S. Geol. Surv. Professional Paper no. 19, p. 18, 1903. 4 Calkins, F. C., U. 8. Geol. Surv. Water Supply and Irrigation Paper no. 118, p. 35, 1905. 258 University of California Publications in Geology [Vou. 10 The collection from the locality near Hanford (loc. 3031) in- cludes the following forms: Megalonyx, small species, probably new. Equus or Pliohippus, caleaneum Camelid, small, near Pliauchenia Camelid, possibly larger than first mentioned form Cervid, antler fragments Leporid, new genus Fish vertebrae and other elements of skeleton Testudo, fragments With the exception of the ground-sloth remains the material from locality near Hanford (loc. 3031) is not well preserved, and this form furnishes the only type diagnostic of any recognized faunal stage. The Megalonyx specimen consists of a well-preserved maxillary with all four cheek-teeth in perfect condition. The species resembles the Pleistocene M. wheatlyi in size, but is probably new. A single specimen representing the horse group consists of a considerably worn calecaneum or heel bone somewhat smaller than the average of caleanea of the Pleistocene horses, and exceeding little if any the average of Pliohippus from the West Coast Pliocene. It is considerably larger than the specimens commonly found in the West Coast Miocene. Of the camel remains none of the fragments can be generically determined with certainty. A portion of a tooth and an incomplete proximal toe bone seem to represent a type not more advanced than those of the later Tertiary. They appear smaller and less specialized than the known forms of the West Coast Pleistocene. Deer are represented by fragments of antlers, some of which show the burr well preserved. The deer of the Pleistocene and later Ter- tiary are not as yet well enough known to furnish a good basis for comparison of the fragments represented in the White Bluffs col- lection. A single upper cheek-tooth of a rabbit-like form obtained in the White Bluffs beds is considered by Dr. Lee R. Dice to resemble in its tooth-pattern a new genus known from the middle Miocene and early Phocene of northern Nevada. In this specimen the enamel folds on the re-entrant angle are comparatively coarse, in contrast to the finer folds seen in the teeth of the later rabbits. The fish and tortoise remains have not shown characters furnishing definite evidence concerning geologic position. 1917] Merriam-Buwalda: White Bluffs of the Columbia 259 The material obtained one to two miles north of Ringold School (loc. 2757) includes upper and lower cheek-teeth and fragments of the skeleton of a horse in which all the characters noted are those of an advanced member of the genus Equus. In the upper cheek-teeth the protocone is long anteroposteriorly, the anterior lobe projects far in advance of the isthmus connecting it with the protoconid, and the inner wall is markedly concave. The fossetts are narrow, and the bor- ders show fairly complicated folds. In the lower cheek-teeth the inner faces of the protoconid and hypoconid are flat. The metaconid-metastylid column is long anteroposteriorly and broadly grooved internally. The valleys anterior and posterior to the metaconid-metastylid column are ‘narrow transversely, as in Equus. The parastylid is short. :..---:- ee 15. Notes on the Later Cenozoic History of the Mohave Desert Region in ‘a California, by Charles Laurence Baker ..........--.:..:<:csc-s--cecscsasesescenenensrcetes 16. Avifauna of the Pleistocene Cave Deposits of California, by Loye Holmes 17. A Fossil Beaver from the Kettleman Hills, California, by Louise Kellogg 19. The Elastic-Rebound Theory of Earthquakes, by Harry paclae Reid ~ VOLUME 7. : r: 1. The Minerals of Tonopah, Nevada, by Arthur S. Eakle ................. ae 2. Pseudostratification in Santa Barbara County, California, by George | 0} 50) anes ene eA SEAL OA GeO OD nee een. Speer NE eS Sn 3. Recent Discoveries of Carnivora in the Pleistocene: of Rancho La Brea, Moerniam= -ix. teu P a Se ea & UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 17, pp. 287-292, 3 text figures Issued May 26, 1917 AN EXTINCT TOAD FROM RANCHO LA BR Q censomian Instif, . BY (oS “% / \ CHARLES LEWIS CAMP (2 JUN 7="1917 2} \ \ Y, INTRODUCTION posits of Rancho La Brea are those of toads. This material includes, besides remains of the species now inhabiting the region (Bufo boreas halophilus), some limb-bones, vertebrae and part of a skull of an undescribed species of toad now extinet. But few fossil salientians have yet come to light, and as the fragile nature of their bones makes it improbable that very many ever will be found, unusual value at- taches to the present collection. The finding in the same Pleistocene deposits of numbers of beetles of a kind often fed upon by toads is significant ; and the discovery of bones of toads in the Pleistocene in as great numbers as in the Recent localities would seem to mean that toads were then as abundant in the region as they are today. The extinet species here described seems closely related to the Recent Bufo boreas, a species ranging along the Pacific Coast from southeastern Alaska to San Diego, California. There is unfortunately some question as to the exact locality of occurrence of the type skull of the fossil toad, and hence as to whether it is really a Pleistocene form; but a parasphenoid from Pleistocene locality 2051 corresponds exactly with the type of the new species, and differs, as does the type, from the single parasphenoid from Recent locality 2052, and from B. boreas. Measurements of the parasphenoid from locality 2052, in addition to other skeletal measurements (see table Il), seem to show that the toad from that locality resembles Bufo boreas more closely than the extinct form. BUFO NESTOR, n. sp. Type specimen, a portion of a skull, No. 22468, Univ. Calif. Coll. Vert. Palae., consisting of all the anterior cranial, otic, and occipital elements intact except for slight damage to the left fronto-parietal. Locality 2051, Rancho La Brea, Los Angeles County, California. eermeene rye ne ‘tig, { M seve He : ‘ : on lai MUSS The only amphibian remains so far discovered in the asphalt de=— 288 University of California Publications in Geology [Vou. 10 Fronto-parietals flat, not fused in. midline, scarcely concave; dorsal surfaces considerably roughened; sides nearly parallel and projecting downward slightly around the cranium. Sphenethmoid relatively large, deeply notched posteriorly, nearly in contact with prootics behind and involving cranium in a more complete ossifi- cation than in Recent toads of related species. Short posterior arm of parasphenoid, pointed ; anterior arm below cranium wider than in recent Bufo boreas; lateral wings below exoccipitals relatively and absolutely wider than in other species of the group; a strong trans- Figs. 1-8. Bufo nestor, n.sp. Skull, No. 22468, * 2. Fig. 1, dorsal view; 8 ) i , 8.4, fig. 2, ventral view; fig. 3, posterior view. Rancho La Brea Beds, California. verse ridge running medially through the lateral wings; a roughened triangular elevation below intersection of wings and shaft; outer an- terior borders of lateral wing not upturned in contact with pedicel of pterygoid. Prooties extensively ossified, longer in proportion to width than in Recent western toads. Squamosals small, triangular, flat and roughened above; lying in the plane of the fronto-parietals and extending out above the prootics about half the length of the latter. Foramen magnum slghtly wider than high; condyles meeting below; extending about half way up sides of foramen and overlapping edges of latter inside about 0.4 millimeter. ‘‘Condyloid’’ foramen relatively and absolutely greater in diameter than in skulls at hand of Bufo boreas boreas and B. b. halophilus. 1917 | Camp: An Extinct Toad from Rancho La Brea 289 North American toads (Bufo) ean be placed in three divisions: the americanus-lentiginosus-cognatus group with prominent angular head erests; the debilis-punctatus-alvarius seetion with crests low and eurved around the orbits and with broad fronto-parietals; and the boreas-canorus group with no cranial crests (except in old adults) and with narrow fronto-parietals. It is to the latter division that the present species seems to belong. Bufo nestor differs from existing Pacific Coast toads, of the forms related to B. boreas, in its wider, flatter and more roughened fronto-parietals; longer and wider sphen- ethmoid; stouter and posteriorly pointed parasphenoid ; flatter squa- mosals; mere slender prooties; larger and more completely protected brain-case. Other material, consisting of toad bones, doubtless of the above deseribed species, from locality 2051, Rancho La Brea, is as follows: Fourteen vertebrae ; 2 third, 1 fifth, and 4 ninth (sacral) ; one pelvis; one ilium; eleven femora; twenty-four tibio-fibulae; fourteen humeri; five radio-ulnae ; two complete and one fragmentary calecaneo-astragali ; and one parasphenoid. In addition to the above, there is toad material, from locality 2052, consisting of seven vertebrae: 1 third, 2 fourth, 1 seventh, and 2 ninth (sacral) ; one ilium; twenty-one femora; thirty tibio-fibulae ; twenty-two humeri; six radio-ulnae; two complete and two fragmentary caleaneo-astragali; and one parasphenoid. The parasphenoid from locality 2051 agrees with the type in ratio of wing width to total length and in the pointed character of its posterior tip. It differs in the above characters from the parasphenoid from locality 2052 and from B. b. boreas and halophilus. Femora from localities 2051 and 2052 and of existing boreas are almost indistinguishable. The largest are only about two-thirds the length of a frog femur of medium size (Rana draytonii), and all bear larger epiphyses than do corresponding bones of a specimen of spade- foot (Scaphiopus h. hammondii) at hand. The sigmoid curvature is more pronounced than in Bufo woodhousi. The smallest femur, from locality 2052, is much shorter than in Hyla arenicolor, but is thicker through the shaft. The largest specimens are longer than in any B. b. halophilus at hand and approach B. alvarius, but differ from that species in the more flattened character of the median ridge. uaprsed o 0" 0 "TO ‘068T “ON snypry doe “Fe v ‘QIPPIL BALTIIG 19 suprydorpey “q * o} ‘WaA “SUIT ‘BEE “Fue ‘[00Z7 T6L 9ST Sor O'CE 9°61 9°96 8°0E SOG ABRIOry (j) snprydopey “q “gq volg vy OyouResy OVE Ong 6F te HE 9'8L FSG Gel ost G86 9G 6 SG OTS ete CoG ary ‘1OJSou * TSGO% Ajtpvoory ‘Ww alg ery oyoury ‘ds e re apt YIPTA 1230} 0} SurM Fo o1yey ae YSU] [BJO} OF SUT JO YIPIM Jo oey ~~ YJSU9] [8}O} 03 WIR IOLIOZUB JO YIPTIM Fo o14ey Sepaig Bae ATG ee UWINI[I JO Y}Sual 4Sozvoid 0} WNIT Fo (FYSIoY) oJoWIVIP WNWIXBU JO O1ZRYy Saag apse = uouttdeds ouo ‘uMTTT Jo YASUI, 4So}BIIH ~~ qourrdeds oo ‘UIMT[L FO JYSIOY IO YZpPTM 4ysoyVaty ape ay uouttdeds ouo ‘Y}PIA [VUIPNyLsUOT JSoqyvory ee eec gee ope ae tawtdeds ouo ‘YAduaT 489}BI.0 Bret? tha" 1a a aaigligpeanc eR uouttveds oo ‘YySUVT [VIOY, - suourtsods vaig vy JO Jsosuol Fo YYSuaT suouttoeds Bolg BT FO 4SojIoYS JO YySuaT --~ suoutoads valg Bry [[B JO oSVIOAV ‘YJSUIT [VIO Sarita anges suouttoads Borg VT JO JSesuol Fo YAduaT cacraparacaae suauttoods valg evry JO ysoqyloYys Fo YYduT eas suouttoods volg VT [[V FO svIOAV ‘YASUI, [BIOJ, meena a stouttods vaig vy FO JSosuoy, JO yASsueT egies saat suoutoeds vorg vy FO 4JsoJLOYS JO YYSGuaT ae suouttoods Bolg VT [[@ JO osvIOAR “YASuT [BIO J, Sea a suowtods voig vy Jo ysosuoy, Jo ySsueyT ~ suouttoeds Bolg BT FO JsoJLOYS FO YYduT es suowtoods vorg Bry [[@ FO 9svAIOAV ‘YSU, [BIO JUIMIANS BOTT prousydseieg prouoydseieg prouoydseieg SIA[Og STATO SIA[Og wNLDeg WNIBg snyeseryse -OOUBI[VD ‘Buln-oIpey Buln-oIpey vupn-orpey Sn.ALOUIN FT SnaoUtn Fy snow yy BNGY-Orqyy, BlAdy-Orqny, Bag y-Orqny, INU if INWd iT IMUw9 J au0g SUMLAWITIUPY NI ONG AO SINAWAYASVAYT IVLATENG IT ATaVa 292 cs ny: At NA OF THE SANTA MARGARITA BEDS IN aga _ THE NORTH COALINGA REGION ee Soe OF CALIFORNIA a6) Ase et Lae BY : qqsonlan lnstiz, ie * JORGEN O. NOMLAND Ne 3 “ooe my NOV 22 1917 me “tional muse 4. pee ir aye = UNIVERSITY OF CALIFORNIA PRESS E 5 _ BERKELEY . 3 eations of learned societies and oor rpae ‘uni all the publications of the University will be sent upon publications and other information, address the Manager California, U. S. A. All matter sent in exchange should Department, University Library, Berkeley, California, U. S. A. Orro HARRASSOWITZ LEIPZIG a1 Agent for the series in American Arch- Agent for the series aeology and Ethnology, Classical Philology, aeology and Ethnology, A Economics, Education, History, Modern Botany, Geology, Mathe Philology, Philosophy, Psychology. ; Physiology, Zoology, and Memoi Geology.—ANbRrEwW C. Lawson and JouN C. Merriam, Editors. Price, volume volumes 8 and following, $5.00. SS Cited as Univ. Calif: Publ. Bull. Dept. Geol: Volume 1, 1893-1896, 435 pp., with 18 plates, price ~ Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price .... Volume 3, 1902-1904, 482 pp., with 51 plates, price Vclume 4, 1905-1906, 478 pp:, with 51 plates, price .... Volume 5, 1906-1910, 458 pp., with 42 plates, price -...........---..2-ece-eceoeoe A list of titles in volumes 1 to 5 will be sent upon request. VOLUME 6. . The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller........... ra 2 . Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern Nevada, by John C. Merriam. Part I.—Geologie History............. ‘5 The Geology of the Sargent Oil Field, by William F. Jones .............. . Additions to the Avifauna of the Pleistocene Deposits at Fossil Lake Loye Holmes: Miller <2. 2 5 sonics cdicstees tanen enn cnedatons Seotectenn cock 5. The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Ri 6. Note on a Gigantic Bear from the Pleistocene of "Rancho La Brea, by Jok oA Merriam. < 7. A Collection of Mammalian Remains from Tertiary Beds on the Mohave De by John C. Merriam. . es Nos. 6 and 7 im OM€ COVED... neceeneeennneoneneenneetennenacenteecmeenenacenacnenas PO pr and Tejon North of Mount Diablo, ee Roy E. Disketen Apes 9. Neocolemanite, a Variety of Colemanite, and Howlite from Lang, Lc County, California, by- Arthur S, Eakle 2.2 /<. 38... eee 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. Nevada, by John C. Merriam. Part Il.—Vertebrate Faunas ..... 12. A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, aig 0 NS ieee een ae seis eee arent Sipe Uae a : 13. Notes on the Relationships of the Marine Saurian Fauna Described from | of Spitzbergen by Wiman, by John C. Merriam. 17. A Fossil Beaver from the Kettleman Hills, Cal faruiae by Louise rae 18. Notes on the Genus Desmostylus of Marsh, by John C. Merriam ......... 19. The Hlastic-Rebound Theory of Earthquakes, by Harry Fielding Reid VOLUME 7. 1. The Minerals of Tonopah, Nevada, by Arthur S. Eakle ...._... : 2. Pseudostratification in Santa Barbara County, California, by Gaoree Dare he — 2 oye A eecB pec scech a neat tae co wacs ote eae sea eo ee 3. Recent Discoveries of camae in the Pleistocene of Rancho a Meerrie rns noeS oan cee ae en Ta Clarke. 34 2, ape ee eee ee Scenes, 5. Contributions to Avian Palaeontology- or t i Toye Holmes Miller sae 2s eee UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 18, pp. 293-326, 2 text figs., pls. 14-20 Issued November 8, 1917 FAUNA OF THE SANTA MARGARITA BEDS IN THE NORTH COALINGA REGION OF CALIFORNIA BY JORGEN O. NOMLAND CONTENTS PAGE TITAN OMAN 1, ern ee ac re ee 294 Previous palaeontologic and geologic Work -.........22...2..22:..2.:-20e--sceecceeeeeeceneeeeeeeeeeee 294 HvelattonetoO Ober LOLMAtLONS .2cec.0n.s.2.-bccevetetececeesecssacseceesends cccccsececessseetecctecereecececse 296 Lithologie section of the Santa Margarita northeast of Coalinga .................... 298 Fauna of the Santa Margarita northeast of Coalinga ........2..2..2..2..2.22---21-00---+ 299 Other Santa Margarita localities compared ....2......22..22..22:c2:cc2cceeceeeceeeceeeeeeeeeeeeeeees 302 HAR Cif OTUMPEL IN Spy omntee sethantes cence Se OU eure tance As ve cy ce eeecs see beneeedcelesesnies scene 302 ROE. TO ARBUSS CO) STE YG I ees a See eee 302 Pcl Na US mn Viel ll Ciyaae se emcees Mae cretes cc sock ee shit Peco ost eos e oN C cs Snax cs tees cceteopsconcicsocsesscbsachebeeeetes 304 DES CUANUIOTIMOLMS I CCT CS pesce tetera coe he es tees ce sdce cas cedeueessrescue ses scetcesubaceaceissdocetesseansaceveecesceze 305 PACE AINIGIS MC OM MAUS | oY SY costs tere svete eae aren ee enee uae se cesteateece ceases 305 Chioness emmplicatuss Mas ye ce coe cos Oeste cee cei ts eee Seen eee: ease 305 OStreambibamaconcu satay Mey vals e-cccesccsc-cet sce cceucseceeeeeecee ees eese cee eeezeceeccvee---ceees= 306 IPECLEM (CLASSICALGO DILOKMAtUS, Ny VAN o.-2a-.2--2cqnc-cc-seeeeececee eeececcneeceeecneeoenensenee 307 Herel LO Mma ECL AT Kasay SPs erescfeeeeacees face ved satscebese=tecceeceseveccsdensaeetuceeeceuseesoicet dea dete 307 TE SATAN Ae YOR SH EEN 21 515 {55 Of paso eee See ee 308 Mepuihere Marr arwtanas, Mey Sp. pesca cee se vonkeecce oeee cent sccn- Seeecencuseccesectca owastatetscesess 308 Acanthinam(@MOnoceras)) MOMMA, Ne SPse .--peseqe---naeecee-ee-ceecseeeecaseeesecceneecesceseeeee 309 WEIS UML S petal Ml alt OVmId tS Poy sec. c eee ezes seb resetceeseBevece cueseocdvens-cv-cest 2 -chatuseassevcsea tenons 309 HER UANG YOUN eine VAT TAs eT SYP ce cc ste eevee eee ces ance eet cacnceccsd cstdteeionenseensiesctecepsceseessfo-c 310 HRC CUA MUN CAMMY SD ey scetedcvecetec.tc2-s.es-cascuce—cs.cstepeccocalnsvecatseseds-ccctsessececcesSceeurcssesencee GUO MRC OU AR RV ATS CTLAWA) © Megs [ue ceeces see c Sco seseczatc. soeeed au teeu et eae Sessdeseccsancesmeeseesecddi ons 311 HM MOWMONMPeTClLE PANS WASPS 22.2cseecsceeeced sete ewes coeeecetacce eer eecaese-asctectenenccuseseenacee 311 MNP LOLA CVVAneIN SP saree cece a tee sca ete cee neces scoters ea ccc asac siete deeds as cdeecedesenss 312 MMIMTUGella MAT CAVUCAN Asp TIS Die cc: coenteccec-cactessascessousceseestersteettbeseas isteacenseserceveesiie 312 2.94 University of California Publications in Geology [Vou. 10 INTRODUCTION Since the first description of the Santa Margarita in the San Luis quadrangle by Dr. H. W. Fairbanks, the question of age of this formation has from time to time attracted much attention. Especially important has been the relation of the Santa Margarita to the upper Miocene and Pliocene formations in the vicinity of San Francisco Bay. The Santa Margarita was considered by Fairbanks a division of the San Pablo, while a number of other geologists have thought it older than that group. The preservation of the fossils of the Santa Margarita at the type locality is very poor. Few attempts have been made to list a typical Santa Margarita fauna, and correla- tion with other localities has been uncertain or frequently impossible. A study of the Santa Margarita fauna has therefore become highly important for correlation purposes. The present paper is a study of a fauna collected from beds in the north Coalinga region which have been correlated with the Santa Margarita. The palaeontologie studies apparently indicate that these beds represent the upper part of the San Pablo group. The faunas also indicate that they represent at least in part the same horizon as the Santa Margarita at the type locality. Most of the material studied from the Coalinga region was col- lected by Dr. B. L. Clark during his research on the fauna of the San Pablo group. The writer is much indebted to Dr. Clark for the use of his field notes on the geology and for numerous valuable sug- gestions, especially in regard to correlation with the San Pablo fauna. Dr. R. E. Dickerson kindly permitted the writer the use of material in the collections of the California Academy of Sciences, San Fran- C1Sco. Previous PaLAEONTOLOGIC AND GEoLogic WorK The first published account of palaeontologic and geologic investi- gation in the region north of Coalinga was included in a paper pub- lished in 1905 by F. M. Anderson.t. In this publication the Santa Margarita was grouped with what he called the Coalinga Beds. These beds comprised what was later mapped as Vaqueros, Santa Margarita, and Jacalitos formations by members of the United States Geological Survey. A brief general description of the geology with faunal lists 1 Anderson, F. M., A stratigraphic study in the Mount Diablo Range of California, Proc. Calif. Acad. Scei., ser. 3, vol. 2, no. 1, 1905. 1917] Nomland: Fauna of the Santa Margarita Beds 295 was given. The age of the beds corresponding to the ‘‘ Jacalitos’’ was regarded as uppermost Miocene. In 1908 Anderson? published another paper including a descrip- tion of the same region. The term Coalinga Beds was then modified so as to comprise a part of the ‘‘Jacalitos’’ and the Santa Margarita above the lithologie member called the Big Blue. It was suggested that the Coalinga Beds might be the equivalent of the San Pablo in the northern part of the Mount Diablo Range. In the preliminary report on the Coalinga district by Ralph Arnold and Robert Anderson? in 1908, the Coalinga Beds as defined by F. M. Anderson were divided into Vaqueros, Santa Margarita, and Jacalitos formations. The name Santa Margarita was used _ be- cause of the similarity of the fossils to those occurring in that for- mation in the San Luis quadrangle in San Luis Obispo County. This formation was believed to be of upper middle Miocene age. The Big Blue was tentatively included with the Santa Margarita. In a bulletin by Ralph Arnold* on the palaeontology of the Coalinga district, a short list of species found in the Santa Mar- earita was given. The formation was believed to be at least in part older than the San Pablo. The latest report on the geology and oil resourees of the Coalinga district by Arnold and Anderson’ does not differ essentially from their earlier reports on this region. It includes a general discussion of both the palaeontology and geology. In the study of the palaeontology of the San Pablo group, B. L. Clark® compared that fauna to the forms found in the Santa Mar- garita. It was shown that nearly one-half of the species found in the Santa Margarita also occur in the San Pablo. It was also stated that this formation was the equivalent of only the upper part, the Astrodapsis whitneyi zone, of the San Pablo. A historical summary of the literature dealing with the San Pablo-Santa Margarita was included. 2 Anderson, F. M., A further study in the Diablo Range of California, Proc. Calif. Acad. Sci., ser. 4, vol. 3, 1908. 3 Arnold, Ralph, and Anderson, Robert, Preliminary report on the Coalinga Oil District, California, U. S. Geol. Surv., Bull. 357, 1908. 4 Arnold, Ralph, Palaeontology of the Coalinga district, Fresno and Kings counties, California, U. 8. Geol. Surv. Bull. 396, 1909. 5 Arnold, Ralph, and Anderson, Robert, Geology and oil resources of the Coalinga district, California, U. 8. Geol. Surv. Bull. 398, 1910. 6 Clark, B. L., Fauna of the San Pablo group of middle California, Univ. Calif. Bull. Dept. Geol., vol. 8, no. 22, 1915. 296 University of California Publications in Geology (Vou. 10 The most recent report on the geology of this section of the state is on the region north of the Coalinga district by Robert Ander- son and Robert W. Pack.‘ The Big Blue is not ineluded with the Santa Margarita, but is regarded as Vaqueros, this being based on fossils found in the region studied. The Santa Margarita is consid- ered older than the San Pablo. RELATION TO OTHER FORMATIONS The Santa Margarita formation of the San Pablo group as mapped in the Coalinga district is found in two areas. The lithology of these two regions is decidedly different. West and southwest of Coalinga the formation consists almost entirely of a light-colored diatomaceous shale. This shale in many characteristics is very similar to the Monterey Shale found in many parts of the Salinas Valley. At some localities west of Coalinga a thin basal sandstone is found con- Qal SS" IS Horizontal Distance represented aboul 4 Miles Fig. 1. Generalized section across formations on east side of Diablo Range, northeast of Coalinga. IKck, Cretaceous; Ttj, Tejon (Eocene); Tel, Oligocene; Tt, ‘‘Temblor’’ (Miocene); Tsm, Santa Margarita (Miocene); Te, Etchegoin (Pliocene); Tpr, Tulare (Pliocene); Qual, Pleistocene and Recent alluvium. (After Ruckman.) formably below the shale. From this member a small fauna has been obtained, which is the chief evidenee favoring inclusion of this sand- stone and the shale above with the Santa Margarita. The shale west and southwest of Coalinga rests with large discordance in dip on the Vaqueros and is overlain uneconformably by the Etchegoin. In the other area which is found north and northeast of Coalinga, the Santa Margarita is lthologically quite different from the diatomaceous shale. The formation here consists entirely of soft yellowish sand- stone which in many localities is highly fossiliferous. It is the fauna obtained from this area of Santa Margarita which will be described in the present paper. As shown by the mapping of the region north of Coalinga by 7 Anderson, Robert, and Pack, Robert W., Geology and oil resources of the west border of the San Joaquin Valley north of Coalinga, California, U. 8. Geol. Surv. Bull. 603, 1915. 1917] Nomland: Fauna of the Santa Margarita Beds 297 Arnold and Anderson,* and by Anderson and Pack,’ the Santa Mar- garita sandstone is continuous as a thin series of beds flanking the eastern slopes of the Diablo Range from near the town of Oilfields to a short distance north of Arroyo Honda. The formation is thus exposed for a length of somewhat more than twenty miles, being apparently overlapped in both the northern and southern ends by the younger Etchegoin. Another small exposure of the same forma- tion composed of fossiliferous sandstone is also found a few miles northwest of Coalinga. Considered as a whole, the Santa Margarita is decidedly distinet from the adjoining formations. At some localities, due to the simi- larity of lithology of the Santa Margarita near the base of the underlying lithologic member ealled the Big Blue, the line of con- tact is traced with difficulty. The Big Blue was therefore tentatively mapped with the Santa Margarita by Arnold and Anderson. The more recent work of Anderson and Pack?! in the area north of the Coalinga district has shown that the Big Blue belongs with the Vaqueros and that it is unconformably related to the Santa Mar- garita. The Big Blue consists largely of deposits of serpentine detri- tus in part at least of land-laid origin. In the Coalinga district it is highly colored and is barren of marine invertebrate fossils. In the area north of the Coalinga district, however, Anderson and Pack report the finding of marine fossils in this member. The Santa Margarita is similarly decidedly distinet from the overlying Etchegoin. As already stated by the writer elsewhere," there appear to be good reasons for believing that the contact between the Santa Margarita and the Etchegoin is about two hundred feet stratigraphically lower than the Lne mapped by Arnold and Ander- son. The beds containing fossil remains of the Pliocene horse Neo- hipparion molle Merriam would thus be included with the Etchegoin instead of the Santa Margarita. This will therefore be used as the base of the Etchegoin in the present paper. As thus defined, the beds lying immediately above the Santa Margarita have a number of characteristics indicative of terrestrial deposits. These beds are 8 Arnold, Ralph, and Anderson, Robert, Geology and oil resources of the Coalinga district, ete. 9 Anderson, Robert, and Pack, Robert W., Geology and oil resources of the west border of the San Joaquin Valley, ete. 10 Op. cit., p. 92. 11 Nomland, J. O., Relation of the invertebrate to the vertebrate faunal zones of the Jacalitos and Etchegoin formations in the north Coalinga region, Califor- nia, Univ. Calif. Publ., Bull. Dept. Geol., vol. 9, no. 6, 1916. 298 University of California Publications in Geology (Vou. 10 highly colored, contain a large amount of silicified wood, leaves, and, as stated above, remains of land mammals. As will be shown by a study of the accompanying list of species, faunally the Santa Margarita differs markedly from both the Vaqueros below and the Etchegoin above. Only a few of the species are found in the adjoining formations. The nearest correlative of the Santa Margarita appears to be the upper part of the San Pablo group’” as developed in the northern part of the Diablo Range. LirHouoeic SECTION OF THE Santa Marcarira NorTHEAST OF COALINGA The sandstone member of the Santa Margarita as exposed in the area northeast of Coalinga was probably deposited, unlike the adjoining portions of the Vaqueros and Etehegoin, entirely under marine conditions. The following tabulated section indicates in a general way the lthologic character of the formation. It is to be See 2 RD 2 8880.3 0a °S°O oS Fig. 2. Detailed section across the Santa Margarita about ten miles north- east of Coalinga. Horizontal distance about 2500 feet. (After Clark and Ruckman. ) borne in mind, however, that the beds vary greatly within a short distance and that the section can be applied in detail to only a very limited area. DmraILED SECTION OF THE SANTA MARGARITA TEN MILES NorTHEAST OF COALINGA Etchegoin Feet Basal gravel with silicified wood and gypsum. MNeohipparion molle found short distance above base Santa Margarita Gray thin-bedded sandstone with well-rounded pebbles of brown chert, Quartzite wand Martz smOnZ Onn Geyser esceeeeseeeesee cece meas eee daven sae seeae te cneeseraes 2 Buff to white, well-rounded, medium to coarse-grained sand ................---- 18 Hard, coarse, quartzose sand with pebbles of quartz monzonite, andesite, and rhyolite; icement calcareous izes.sssecete-ceeteeseets seat ee seseeeeecaeeeteesnes. ena 13 White to bluish-white, incoherent sand consisting chiefly of well-rounded Quartz; Srains: 22... ees ie 50 Fossiliferous grayish-brown sandstone with well-rounded grains of quartz sand feld spay 2.2.22. 2cc.-sceecta--cdeeseseee eee ee 25 12 Clark, B. L., Fauna of the San Pablo group of middle California, Univ. Calif. Publ., Bull. Dept. Geol., vol. 8, no. 22, 1915. 1917 | Nomland: Fauna of the Santa Margarita Beds 299 Feet Hard grayish-brown sandstone; grains moderately well-rounded with MED OLES OL mV OUCATI C210 CKSisescteeseq nse cee stececssenenec ts eeesc-nectcesereeescsceeseeam ieee eseess 13 Barnacle reef, with arkose sand and large number of specimens of WES CULTS sree aes eu tact seats gO econ sae wa fees sts Sa ce aca es on tere anti race one ceatec seve ree eres 1 Coarse, light-gray, pebbly sand with calcareous cement; pebbles sub- angular, chiefly andesite, quartz, and feldspar; fauna includes Astro- QD SUS OMTMOUGI a OSUTGC. UD CSDCTUUT st eee case ate tea eae eee 30 Incoherent fossiliferous sand with large number of well-preserved speci- MOVOTO eg eLC Ui0LU SC CAL) pee te ee eg aw Be eee 38 Bedvot Osined titan im) ashy Sand iss es aesce cess ce cece nscecese corsa cess seat eee Sune “aShy | Sar cxcsoccvecsceve loses sevesevescctesecssdese2es ceececcccesyseeasstescesssescessateseaccstatestecs 25 Mintaceous eSamd witht OSUCON UVC C1 scesecescec:peccteenermaeeenaeee ee ee 50 16. Avifauna of the Pleistocene Cave Deposits of California, by Loye Holmes Miller .... 17. A Fossil Beaver from the Kettleman Hills, California, by Louise Kellogg ................ 18. Notes on the Genus Desmostylus of Marsh, by John C. Merriam .............02..-2 19. The Elastic-Rebound Theory of Harthquakes, by Harry Fielding Reid)... - VOLUME 7, = | 1, The Minerals of Tonopah, Nevada, by Arthur S. Eakle ... a. csseessesesecrneere Seaksteeauee 2. Pseudostratification in Santa Barbara County, California, by George Davis Louder- WO. Ce oie can cos cnsnceseocnstagseccseweretcnccdisebba psturessonapeseesncs erasenaessiaeaee eee tage cn ee a ae 3. Recent Discoveries of Carnivora in the Pleistocene of Rancho La Brea, by John | Mierriar © 2.220. ors lcdece dan Recto ccc cepts Bees Se aoa Se 4. The Neocene Section at Kirker Pass on the North Side of Mount Diablo, by TC ark oo nnacit ate nstbcades casnctnccconderonacenesulsuitna dient aoee as ayea se Sa SgaeeS aaah Soa er 5. Contributions to Avian Palaeontology from the Pacific Coast of North Ameri a, } - Loye Holmes Miller sescitorsoen: evens snensfancienazeir ud aeusostns = eee haa Mtensey cateel Nath oh nee septa ‘ 3 4 Fin ae UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 19, pp. 327-360, pls. 21-24 Issued October 17, 1917 MINERALS ASSOCIATED WITH THE CRYSTAL- LINE LIMESTONE AT CRESTMORH, RIVERSIDE COUNTY, CALIFORNIA (25 BY \ ARTHUR S. EAKLE CONTENTS PAGE DOS Cre LO TMO LUC) LOCKS Meces tessa steerer acces eee gee coast tecadscvcczeecpouecgesceues-cesescete roses: g0nss 328 Igneous intrusives and metamorphism ........22..2..22-.22---2c2sceeceeseeeeeeceeeeeeeeeeeeeeeee 328 TEUHDRSS, GepaUel Ca ue ys VSN eee ee a eee A are eae ope eS 329 TUS aH EGU VSS). TROL ONS a rn Oe ee 329 ADVENT cae AC eae eg 330 Mietamorphism Of the ImMestome! 2i..222.22-ccccce.ceccnence-s¢eceeececee-eeeeecnecceeceecetenoteee 331 MCS cmp bLOM OL diG WWE ANS 22. c aoe ecco cece se ee cca se ev ceneeeee eencenvencepeceasiwsascesseseeses GOL Minerals disseminated in the white limestone of Chino Hill ~......00..2........ 332 J BNE UUCR Be) aa ee ae ee ee 332 Hetay, Clit, OTA ONC SI Ge waren see rs er 2 es eee ot eae 333 (EVO TIGA © CUiit eee etree he ence teens tee, ee ene oes 2 ee ee eee eo ee 333 (GTR 0) CE SY Gee ag ee ee ae ne ee 333 TBA a GYRO Oo) esse ee ae yn ee Ue ep ee 334 SSIES OER ENS a re ee ee 334 Minerals in the contact zones of Sky Blue Hill ................02.20.2..22-21220e1eee ees 334 HSE MECN) Cit eer eee came meer rs ener SI ee Pr ee oe a ecg ee setae ee ee 334 WVU ONO ) a a es ra ne eee o ee eee ee eee ft ee es 334 AVE SUwval au viiits ememrennem emcee ater erect NENG Bie a SR he Sei weet haususbzad obec 338 (GRY bare ae eee eee ee See we one ne Mae Ae rec ek he letectone asses eeeat ene seegaceeeate meas 339 VDI OSG oh, ee ee ra a ee er ere ea 340 EXCA MIU MOP INNYAUGE suevicllig, WSU ULC WALt CU sees ae ee sete eons e eee ce eee teen nc cecaeenctstencee ene sease 341 Vito mnited Ge Dt Ge cere see arene eet RE cee ue he Pose Rca ate e te e ney ev vente oreean cas itteee 342 NATE EMH SY Fa are a a PE 343 @restmonreite yaa meyye min Oral ecc2ic, cece score c.ceee cece ces ceeceesedec esta sesccaenace-esease~s ee 344 TRAVEL SLCCLLC eaR Me Wi IMIMeCT AN 2-28 c. otc et cee eter cnen tees ses teube eaeepee eee . 347 CA Tay oo 9 AN ee ee Pe 348 NT OPEN ESTES) esa ae a 348 JaNGMEENFER OS CUES) eae ee ea 348 328 University of California Publications in Geology [Vou. 10 Minerals associated with the intrusives SY eG sy OF if ce epee cere eee yor oe PANU CG eeeeeeeeee : Hornblende and biotite ~........2..0...-..2........ ents curs © aie ease eee PARQ erp Hipidlotenzceseess @ Wat Zao ARopobavovery ib ey ae eee PND GUAM S) epee ee ee Datolite -......... Seapolite ........... Apophyllite Okentte 2222.22 Prehnite .............. Laumontite -........ © alligeeeeeeereee LeU Golauitelies vaabiayepte ls) Spee ee ee Oxydation products DESCRIPTION OF THE ROCKS IGNEOUS INTRUSIVES AND METAMORPHISM At Crestmore, about eight miles westerly from Riverside, there is an isolated mass of granodiorite with a capping of crystalline limestone which is of exceptional interest because of the many minerals developed in the limestone by contact and hydrothermal metamorphism. The Riverside Portland Cement Company’s plant, situated at the base of the hill, uses both rocks in the manufacture of cement. The extensive quarrying is rapidly destroying the hills, and the different minerals and associations almost daily brought to view are immediately earted to the rock-crushers, so that a vast amount of material of scientific value and many fine specimens are lost. The writer visited the quarries a few years ago and collected much of the material described here, but no detailed study of the deposits was made and no opportunity has presented itself for a second visit. Specimens have been collected by others and sent to the University, which have been of great help in making the list complete, and special thanks are due Mr. L. J. Childs of Rialto. He has kept in touch with the quarrying and collected minerals that otherwise would have been lost, and these with notes of their occurrence have been given to the writer. About fifty minerals are described in this paper, but these represent only a portion of what probably could be found by daily 1917] Hakle: Minerals Associated with Crystalline Limestone 329 visits. The cement contains the calcined remains of many beautiful, rare, and perhaps new, mineral species. Hills and Quarries.—The Crestmore limestone forms two hills closely connected by a saddle-ridge. Both hills rest upon a common base of granodiorite somewhat elliptical in contour, with its longer axis trending northeast-southwest. The north is called Sky Blue Hill because of its blue calcite; while the south hill, having pure white marble, has been designated Chino Hill. Sky Blue Hill has a large quarry on its northern side ealled North Star quarry, a larger one on its eastern side named the Commercial Rock quarry, and between them a third one, the Lone Star quarry, has recently been opened. Chino Hill has one large quarry on its southwest side, and the accompanying view (pl. 21) shows this quarry and the plant of the cement company. The floor of the quarry marks approximately the juncture of the igneous base with the limestone capping. The lhmestone forming the capping is a small remnant of a more extensive body of limestone which formerly covered this region. There is a larger mass similar to Crestmore about three miles west, and Slover Mountain near Colton may be another remnant left as a capping upon an intrusive mass. Intrusive Rocks.—There are three types of igneous intrusives oceur- ring in the hills and all three have been active agents in the meta- morphism of the limestone. Granodiorite, quartz-monzonite porphyry and pegmatite are present and intimately associated with the contact phenomena. The granodiorite is a hornblende-biotite rock with a fairly coarse granitic structure consisting essentially of orthoclase, plagioclase, hornblende, biotite, and quartz. The orthoclase, which appears to constitute the main portion of the rock, is mostly white, and the rock is consequently gray as the prevailing color, but patches of brick-red orthoclase oceur, giving the rock a red color. Labradorite and oligo- clase are the triclinic feldspars present, but very little albite twinning is seen. The rock is not fresh and all of the feldspars are muddy and opaque. The dark silicates are mostly black hornblende, which is dark green in thin section, and a few plates of biotite. Quartz is much subordinate to the feldspars in amount. This granodiorite is used by the company as a substitute for clay in the cement. Daily analyses of it are made and three of them will serve to show the relative proportions of the bases. 330 University of California Publications in Geology [Vou. 10 SiO, 60.60% 60.78% 60.30% Al,O; 16.61 16.04 16.03 Fe.O, 5.03 4.82 4.19 CaO 7.93 8.22 7.19 MgO 2.08 1.99 2.26 Loss 4.79 4.75 4.42 97.08 96.60 94.39 The alkalies are not determined in these analyses. Probably some potash and soda have been leached out in the alteration of the feld- spars. The granodiorite has its best exposure on Chino Hill and is plainly seen underlying the white limestone. The rock is mined by tunnels into it from the side of the hill below the limestone. The quartz-monzonite porphyry forms dikes and laccolithic-shaped masses in the lmestone of Sky Blue Hill. The rock is very fine- grained, almost felsitic in character, with an ash-gray color. Under the microscope it is essentially a fine granular mixture of quartz, orthoclase and plagioclase with occasional large plates of feldspar and augite. Some pale green and slightly pleochroic hornblende is present, but most of the dark magnesian mineral is augite. It occurs in granular aggregates of a pale bluish-green color and shows no pleo- chroism. Titanite grains are common in the rock. This rock forms a wide intrusion into the limestone of Sky Blue Hill, since tunnels run into the hill from the floor of the Commercial Rock quarry penetrate it for several hundred feet. It has been the most active agent in the formation of the metamorphic minerals of this hill. The pegmatite occurs as intrusive dikes but it is difficult to trace out their boundaries. They appear to be associated more with the meta- morphic masses of vesuvianite-garnet rock. The pegmatite consists mainly of white orthoclase and green epidote. Orthoclase occurs in large cleavage masses and is usually pure white in color. The epidote penetrates the feldspathic mass in long slender crystals, most of which are altered to a bronze-brown color. Quartz occurs as smoky granular masses but is not prominent. Zircon, tourmaline, axinite, pyroxene, and a few other minerals are occasionally found as accessories and some minerals have later been developed in the pegmatites by hydro- thermal metamorphism. The Limestone.—Daily analyses are made of the limestone and that from the Chino quarry has the following average compositions: 1917] Kakle: Minerals Associated with Crystalline Limestone gall SiO, 4.50% 4.68% 4.26% 5.24% R,0, 1.20 1.24 1.66 1.40 CaO 50.78 50.85 50.00 50.33 MgO 2.50 2.25 2.54 2.60 Loss 40.60 40.36 41.54 40.40 99.58 99.38 100.00 99.97 Analyses show that about two and one-half per cent of magnesia is the average amount of that oxide in the white limestone or marble, and it is therefore not very dolomitic. Associated with, and merging into this rock are masses of similar white crystalline limestone containing much magnesia, as the mineral brucite, disseminated through it in pisolitic-shaped inclusions. The brucite rock apparently overlies the other limestone, and is seen very prominently on the south end of Chino Hill and near the surface in the Commercial Rock quarry on Sky Blue Hill. It may be a remnant of a separate and distinct bed of magnesian limestone, but the amount of the brucite varies consider- ably and it has evidently been formed from some other magnesium mineral, whose origin was due to contact metamorphism, and the source of the magnesia might have been in the solutions accompanying such metamorphism. Metamorphism of the Limestone.—The two hills are utterly dis- similar in the effects of metamorphism. The limestone of Chino Hill was converted into a white marble with very little development of included metamorphic minerals. It does not appear to have suffered successive metamorphism and reerystallization as would be induced by later injections of igneous rock, and the original intrusion of the granodiorite accounts for its simple metamorphism. At the south end of the quarry the rock grades into a brucite-graphite limestone; and the brucite and graphite are so thickly disseminated as to warrant the assumption that the original rock was a highly carbonaceous, mag- nesia-bearing limestone which, by metamorphism, became converted into a mixture of calcite, periclase, and graphite, the periclase subse- quently altering to brucite. The Sky Blue Hill portion of the limestone capping was subjected to later and more intensified metamorphism by intrusions of the quartz-monzonite and pegmatite, and by the hydrothermal action of the silicated-carbonated solutions accompanying or following these intrusions. Practically all of the minerals developed are products of hydrothermal metamorphism. These solutions also carried phosphates 302 University of California Publications in Geology [Vou 10 and small amounts of metallic sulphides. The beautiful blue calcite occurring only in the north hill is a reerystallization by these solutions, and some of the minerals, like the brucite, apophyllite, okenite, crest- moreite, prehnite, laumontite, etc., have been formed by the action of such solutions on pre-existing minerals. Zones or bands of contact metamorphic silicates separate the white crystalline marble from the dikes of monzonite and pegmatite, and some of the material is a compact massive and inseparable mixture. Vesuvianite, garnet, and wollastonite are the abundant silicates of Sky Blue Hill. Plate 22 shows three views of the Commercial Rock quarry on this hill. DESCRIPTION OF THE MINERALS MINERALS DISSEMINATED IN THE WHITE LIMESTONE OF CHINO HILL Brucite—The magnesia hydrate is not disseminated through the limestone as plates or scales but occurs wholly in rounded, pisolitie bodies. The pisolites are generally quite prominent because of their gray, yellow or pink color in contrast to the white calcite. Magnified sections show them to be composed of a congeries of thin, overlapping, curved plates and threads, more or less concentrically arranged, and with a cross-fibered structure. This internal structure indicates great strain and pressure in their formation, and little can be made of them optically. The general interference colors are low, but their com- pressed, interwoven fibrous structure prevents extinction. An analyses of the pisolites gave: MgO 67.48% Fe,O; 0.55 H.0 31.73 99.76 C239 Some of the brucite is deeply colored by ferric oxide, which imparts a yellow and red spotted appearance to the white limestone. Near the surface of the hill in the Commercial Rock quarry, where the brucite has been weathered out, the limestone is cellular, with the cavities lined with the yellow or red oxide. Periclase is assumed to be the original mineral which has changed to brucite by simple hydration. No periclase has been observed and no other mineral occurs in the limestone from which brucite could be derived. The very regular form of the pisolites suggests an 1917] EKakle: Minerals Associated with Crystalline Limestone 333 original isometric crystal with an octahedral shape such as periclase would have had. The internal structure of the brucite clearly indi- cates that they have formed under great pressure, such as would be produced by expansion within a confined space. In a change from the anhydrous periclase to the hydrous brucite an increase in volume of nearly two and one-half times that of the periclase is necessary under normal conditions, and this great swelling has caused sufficient pres- sure not only to produce the twisted and fibrous internal structure of the pisolites, but also to curve slightly the twinning planes of the ealeite bordering the cavities. The names predazzite and pencatite were given to a similar brucite limestone from Predazzo in the classic Monzoni district of Tyrol. Specimens of the predazzite show the same compressed and strained brucites in the white limestone, and they have generally been held to be brucite derived from periclase, and some unaltered periclase has been found. Lanacék' holds from a petrographic study of the predaz- zite that the pisolites are hydromagnesite rather than brucite. Some of the brucite of the Crestmore limestone is altered to hydromagnesite as a later change but the pisolites are in the main brucite, as shown by the analysis. Hydromagnesite—Some of the brucite pisolites have altered by weathering into earthy white material which qualitative tests prove to be the hydrocarbonate of magnesia. It is evidently secondary from brucite and not from any periclase direct. Chondrodite.—This is the only mineral in the list of which there is no well-authenticated proof of its existence in the quarries. Chon- drodite and its characteristic associate, spinel, might be expected among the products of metamorphism in the Commercial Rock quarry, but apparently fluorine was absent, as tests of the spotted limestone which suggest chondrodite failed to show its presence. Specimens of chondrodite have been collected from the Colton limestone. Brucite may form from chondrodite but it much more probable that periclase was the original mineral of the Crestmore rock. Graphite.—The only place in the quarries where graphite is promi- nent in the limestone is on the south end of Chino Hill, in close asso- ciation with the brucite. It is so thickly disseminated through the limestone as small flakes and scales that the rock is of a dark gray color in consequence. The pisolites of brucite are often surrounded by a border of black graphite, probably so oriented by the solutions 1 Min, u. petr. Mitth., vol. 12, pp. 429, 447, 1892. 334 University of California Publications in Geology [Vou. 10 causing the change from periclase to brucite. Graphite was not promi- nent in the quarries on Sky Blue Hill. Phlogopue.—A few flakes of brown phlogopite mica have been observed in the white limestone of Chino Hill. Serpentine.—Very little serpentine has been found on either hill. A few small patches and streaks occur here and there in the white marble of the Chino quarry. MINERALS IN THE CONTACT ZONES OF SKY BLUE HILL Blue Calcite-—The blue calcite occurs only in the Commercial Rock quarry. Some of it is intensely blue, especially when freshly exposed, but it fades somewhat to more of a sky-blue color. It does not occur as one large mass of blue calcite, but rather as seams, bands, and patches intimately mixed with the various metamorphic minerals. When the quarry was first opened the blue calcite was very common and was used for road rock and in sugar refining, but very little is now seen. It is one of the contact metamorphic minerals; and in the reecrystal- lization of the carbonate larger rhombohedrons have resulted, some of the cleavage rhombohedrons measuring four to five centimeters in diameter. The cause of the blue color has not been determined, but is believed to be due to minute inclusions of carbonaceous matter. Slight heat completely decolorizes it. This blue calcite forms the matrix for wilkeite, crestmoreite, xanthophyllite, and monticellite, and contains, besides, minute erystals of vesuvianite and diopside. Pale green and pale pink specimens of calcite are occasionally seen, but the prevailing colors are blue and white. Wollastomte.—The calcium silicate has been most abundantly formed in the limestone, especially on Sky Blue Hill. It forms great masses in the North Star quarry and tons of it can be obtained. Four structural types or habits may be ascribed to the Crestmore wollas- tonite. The first has the common reticulated columnar and fibrous struc- ture which is so characteristic of wollastonite. Crysials of this type are long, narrow and much striated, and generally show no end-faces. Masses of this kind of wollastonite have occasionally been encountered in the limestone of the Chino quarry. The second type is represented by large well-formed crystals having the forms and habit of the usual wollastonite crystals. Glassy white crystals, several centimeters long and more than a centimeter broad, 1917} Kakle: Minerals Associated with Crystalline Limestone 335 occur in direct association with garnet and vesuvianite. They are elongated parallel to the b-axis and have one end terminated by fairly good faces. The forms observed on these crystals are: a (100) m (110) v (101) s (301) e (001) ax (120) a (102) p (111) new g (011) z (320) t (101) The orthopinacoid and base are broad while the domes are very narrow; this gives the crystals an appearance of elongated square prisms. One: crystal had a rough face of the front unit pyramid, which is a new form for wollastonite. Figure 1, plate 23, shows this type. The angles obtained with the two-circle goniometer and those calculated are as follows: Measured Calculated Forms ) p 7) p e 001 90°00’ 5°34’ 90°00’ 5°30’ a 100 90 00 90 00 90 00 90 00 m 110 43 40 90 00 43 39 90 00 x 120 25 31 90 00 25 30 90 00 2 320 55 10 90 00 55 03 90 00 v 101 90 00 45 21 90 00 45 35 a 102 90 00 T9 36 90 00 20 03 t 101 90 00 39 13 90 00 39 35 s 201 90 00 60 03 90 00 60 14 g O11 4 42 46 36 5 39 44 ]2 jo Maul 47 10 53 36 46 29 54 34 The third structural type is granular and very unusual for wol- lastonite. Large masses of snow-white, fine-granular wollastonite occur in the white limestone of the North Star quarry of Sky Blue Hill. The material is loosely coherent and friable; specimens can readily be crushed between the fingers into fine grit and glassy grains. An analysis of this unusual variety gave the composition : SiO, 51.77% Fe.O, 2.12 CaO 44.85 Ign. 1.02 99.76 The general tendency of wollastonite is to erystallize in long columnar forms; when found occurring as a fine granular mass it must mean a peculiar condition of crystallization. Wollastonite usually occurs imbedded in limestone as inclusions, but massive boulders of this granular variety are quarried containing no associated 336 University of California Publications in Geology (Vou. 10 calcite. This friable granular variety has every appearance of having ~ been thrown down as crystalline precipitated granules from a cooled saturated solution of the lime silicate. The precipitate was crystalline as every grain is transparent glassy, but the imperfectly formed crystals were not cemented into a compact mass which would have been ordinarily the case in a dense crystallization such as this implies. Presumably this mass, which seems to be a large segregation in the limestone, was formed by rapid erystallization and sudden precipita- tion from a solution whose temperature was rapidly lowered. This variety is only found on the northern end of the hill and at some distance from the intrusive dikes. The fourth type consists of distinct erystals which have formed by later silica solutions acting upon the limestone in the vicinity of the pegmatite dikes and on the outer border of the contact zones. Acicular and slender erystals with terminations on one end oceur associated with apophyllite and okenite. The crystals are clear and colorless, with bright lustrous faces. By pressure they separate into silky fibers. They possess perfect orthopinacoidal cleavage and have the usual elongation parallel to the b-axis. Twenty-three forms were observed, of which twelve were new, as follows: e (001) y (101) g (011) wu (144) new a (100) r (104) new yp (744) new @ (122) 1 (740) new 6 (104) new o (344) new y (122) h (540) k (103) n (144) new w (142) new q (340) a (102) Dp (744) new e (142) new m (140) new ¢ (101) i (344) new The crystals are slender and consequently the dome faces are nar- row and apt to be striated. The base, orthopinacoid and three domes vat are common to all the erystals. One erystal gave readings for narrow but distinct forms corresponding to two new domes (104) and (104). The end terminations of the crystals are remarkable. The unit prism (110) and elinoprism (120), which are common forms on wol- lastonite, are absent, and a new prism (140) predominates; the prisms (540) and (340), known forms but very rare, are common on these crystals. The pyramidal forms are hkewise remarkable in showing a similar odd series of symbols and no forms common to the usual crystals of wollastonite. Practically all of the pyramids are new forms. The forms (144) and (144) are common on all, with (344) and (344) usually present. Two of the crystals have small faces of the forms (744) and (744). The forms (544) and (544), which 1917] Hakle: Minerals Associated with Crystalline Limestone 337 would complete the two odd series, may also be present, as some approximate readings indicated them, but their occurrence could not be established with absolute certainty. Two very small and poor faces corresponding to the forms (122) and (122) and a line face of (011) occur. The two new forms (142) and (142) were line faces and gave only approximate measurements. Another unique fact about these crystals is that for every positive pyramid there is a negative one with like symbols; but the symbols for the rear faces do not correspond to the front ones. It is characteristic that the crystals have three or four prism faces on their ends each representing a different form. Figures 2 and 3, plate 23, show the combinations on some of the erystals. Figure 3 shows the end of the erystals with the rear faces drawn in the left half in reversed position. Figures 4 and 5 are orthographie projections on the clinopinacoid which bring out better the combination of faces. Only one end of the crystals is terminated, sometimes the right and again the left end. The disposition of the faces indicates a lower grade of symmetry as there is no apparent axis of symmetry, and the erystals could belong to the hemimorphic class of the monoclinie sys- tem, or to the triclinic system. The mineral is strongly tribo-lum- inescent and this physical property is an evidence of a more complex molecular structure. The dome faces on these erystals are identical with those of all wollastonite crystals, but the terminated ends are totally dissimilar. Measured Calculated No. of Forms ~ p p p measurements ce 001 90°00’ 5°30’ 90°00’ 5°30’ 25 a 100 90 00 90 00 90 00 90 00 30 l 740 59 03 90 00 59 04 90 00 7 h 540 49 57 90 00 50 O1 90 00 8 q 340 35 35 90 00 35 35 90 00 10 m 140 13 25 90 00 13 25 90 00 13 v 101 90 00 45 33 90 00 45 33 22 r 104 90 00 18 35 90 00 18 07 i 6 104 90 00 7 41 90 00 7 40 ] k 103 90 00 11 36 90 00 11 56 a a 102 90 00 20 00 90 00 20 00 19 t I01 90 00 39 33 90 00 39 35 24 g O11 5 12 45 44 5 41 44 12 al p 744 60 29 62 19 60 31 63 03 3 o 344 38 59 51 16 39 10 51 19 6 n 144 18 33 45 33 18 40 45 37 11 d 744 58 20 61 41 57 30 60 58 2 i 344 B1 42 48 37 BI 38 48 39 ff 338 University of California Publications in Geology [Vou. 10 Measured Calculated No. of Forms to) p ~ p measurements wu 144 8 09 44 16 7 55 44 19 11 g 122 30 38 47 24 28 57 48 09 1 p 122 T9 02 45 14 20 41 45 58° 1 w 142 15 35 62 51 . 16 05 63 35 1 e 142 Tr 04 62 57 To 41 63 05 1 An analysis of the clear crystals gave: SiO, 50.42% CaO 48.29 MgO 0.60 Fe,0; 0.51 Ign. 0.07 99.89 The optical data were kindly determined by E. 8. Larson of the U. S. Geological Survey: a=11.614; B—=—1.629: y = 1.631; 2H == 98° S505) DVS 35 cet: Y || fibers; Z 1 fibers. Parallel extinction; dispersion per- ceptible p>v. The indices are close to those for pure artificial wollastonite : GAG; f= 1.62075 224 6321, Vi 29" Vesuvianite.—Massive vesuvianite is very common in the meta- morphie zones between the monzonite dikes and limestone. It is in- timately associated with garnet and diopside. Most of this massive variety has a light yellowish color and shows broad crystal faces. Simple crystals of this yellow color are also common, some of them being very perfect. The blue calcite contains crystals of a darker brown color with brilliant faces and somewhat fused appearance. Two general habits of the crystals are prominent. The simpler type consists of the doubly terminated pyramid without any modifying faces on the edges, as illustrated in figure 6, plate 24. Occasionally the edges of these are truncated by the second-order pyramid as narrow faces, and a small base may also be present. The sizes of these crystals range from less than one-fourth centimeter to more than six centimeters in width. All of them are of the light yellow color and they are associated with the white crystalline limestone. The second type consists mainly of the unit bipyramid (111) and second-order prism (100) in about equal development, as shown in figure 7. This type is often modified by very small planes on the edges and on the points of the lateral axes, making a more general combina- tion, as illustrated in figure 8. These crystals have a dark brown 1917] Hakle: Minerals Associated with Crystalline Limestone 339 brilliant surface, with lighter brown interiors, and they occur imbedded in the blue calcite in association with the wilkeite. The small faces grouped about the ends of the axes are often rounded and give readings which yield improbable symbols, but the ones identified are: e (001) a (010) m (110) o (011) p (111) (221) (331) (121) (SE) on ets] y (441) Sen (aleils) i (132) n (154) new D (285)? The new form (154) occurs on several of the crystals; the narrow face of (132) rounded into a narrow face which gives a good reflection and corresponds to the symbol (285), but it is not repeated on any other crystal and must be classed as doubtful. The measured and ealeulated angles are as follows: Forms e 001 a 010 110 011 a 221 331 121 131 132 154 285 28 rsa ce h* xrAK SOK Measured p p 0°00’ 0°00’ 90 00 0 00 44 50 89 50 0 00 28 20 44 55 Bye lal 44 56 56 43 45 00 66 19 26 19 49 56 18 30 59 30 18 31 40 23 11 00 34 30 14 30 41 55 Calculated g p 0°00" 0°00’ 90 00 0 00 45 00 90 00 0 00 28 15 45 00 37 14 45 00 56 40 45 00 66 19 26 34 50 14 18 26 59 32 18 26 40 22 11 18 34 25 14 03 41 34 An analysis of the green vesuvianite by J. B. Wright gave: 36.88% SiO, Al,O; Fe.O, FeO MnO CuO CaO MgO Na.O H,O Gi 336 llyé foul 3.11 0.46 1.50 1.06 33.27 4.73 0.34 0.61 Garnet.—The cinnamon-colored grossularite is abundant in asso- ciation with the vesuvianite. Most of it is compact massive and shows 340 University of California Publications in Geology [Vou.10 only an oceasional broad face of the dodecahedron. Good erystals also occur and some of the rhombic dodecahedrons measure ten centi- meters in diameter. All of those collected are simple dodecahedrons without other forms. Some of the crystals are mere shells of garnet enclosing a center of white calcite. The massive grossularite was analyzed by J. B. Wright with the following result: SiO, 35.53% Al,O, 21.11 Fe,O, 3.95 FeO 0.60 CuO 0.70 CaO 36.06 MgO 0.78 Na,O 0.20 H,O 1.23 100.15 G=3739 Granular yellow garnet and dark brown massive varieties also occur, apparently in connection with the pegmatite dikes. No analyses of them have been made to determine the particular species. Diopside.—Associated with garnet in the zone of metamorphic lime silicates, a deep green massive pyroxene occurs, which is probably a diopside of a darker color than the crystals scattered through the calcite. All of the erystals are of a pale yellowish green color and occur as single crystals imbedded in the blue ealeite. Most of them are small, only a few millimeters long, but some have been found four centimeters in length. They are all of one general type: short prisms tapering off by a succession of unit pyramids to pointed ends, with or without small basal planes. _ Figures 9 and 10, plate 24, show this general habit and some of the combinations. The observed forms are: ¢ (001) e (011) » (331) ad (131) a (100) z (021) o (221) p (121) b (010) vy (221) (Gala) « (211) m (110) w (111) & (aul2)) e (121) nm (231) new The new torm truneates the edge (110) (121) and occurs on several crystals. The edges have many rounded faces and some of the symbols corresponding to them are given unlettered in the following table of measurements and calculations. They are doubtful forms. 1917] Eakle: Minerals Associated with Crystalline Limestone 341 Measured Calculated Forms ro) p cH) p e 001 90°00’ 15°50’ 90°00’ 15°50’ b 010 0 00 90 00 0 00 90 00 a 100 90 00 90 00 90 00 90 00 m 110 43 34 90 00 43 33 90 00 é 001 25 40 32 58 25 43 33 11 z 021 13 29 50 30 13 32 50 29 w lil 55 04 45 55 55 04 45 50 vy 221 49 45 61 40 49 59 61 23 t 112 ap lal 16 51 0 44 16 25 s 111 25 12 33 05 25 07 33 04 o 221 BS 32 55 23 35 22 55 19 rA 331 38 17 66 12 38 19 66 04 a 130 25 27 62 42 25 31 62 58 p 121 35 37 55 29 35 36 55 24 n 231 25 27 62 41 25 19 62 55 e 211 BS 04 45 41 55 04 45 50 e 12) T3 53 50. 27 13 12 50 27 352 20 18 57 07 20 24 57 36 Wino 45 20 55 09 46 11 54 50 836 57 49 29 14 57 32 28 47 14.3.10 69 57 27 41 70 32 27 57 10.12.7 27 O1 48 18 27 04 48 37 NXanthophyllite, var. walwewite-—The rare brittle-mica xantho- phyllite with its associate monticellite from Crestmore has recently been described by the writer,” so only the main facts concerning the min- erals will be incorporated here. Xanthophyllite was first described and named by Gustave Rose* as a wax-yellow mineral in scales and plates, occurring as a constituent of a tale-schist in the Shiskimskaya Mountains in the Urals. Years later the green variety was found and named waluwewite by Kokscharof.* The waluewite or valuevite occurs as a constituent of chlorite schist in the Nicolai-Maximilian mine, near Slatoust in the Urals. These two occurrences are apparently the only ones reported and in both cases the mineral was a schist con- stituent. The Crestmore waluewite is a product of the contact meta- morphism and occurs disseminated through, the blue calcite. Masses of the blue calcite speckled with the green waluewite were once very plentiful at the quarry, but none is now seen. The waluewite occurs in hexagonal-shaped basal plates of a deep grass-green color and vitreous to slight pearly luster. The plates are 2 Jour. Wash. Acad. Sci., vol. 6, p. 332, 1916. 3 Poge. Ann. d. Phys. und Chem., vol. 50, p. 654, 1840. Also in his Reise nach dem Ural, vol. 2, pp. 120, 514, 527, 1842. ’ A fiir Kryst. vol. 2, p. 51, 1877. Also in his Mineral d. Russ., vol. 7, 342 University of California Publications in Geology [Vou. 10 seldom grouped together and they average one-half centimeter broad and four millimeters thick. A few large ones have been found measur- ing several centimeters in width and thickness. While the basal planes are very brilliant the edges are dull, furrowed and impossible to measure. The thicker crystals show polysynthetic twinning like the micas and extinguish in striated sectors. Thin cleavage plates give a biaxial figure with an apparent optic angle of about twenty degrees. Measurements of the optic angle in sodium light showed a variation from twelve degrees to eighteen degrees. The plane of the optic angle is (100) and the mineral is negative. The refractive indices B and y in the basal section are practically the same, determined as 1.660. Several analyses of the waluewite from the Urals have been pub- lished and two of them are inserted here for comparison with the Crestmore mineral. No. 1. Waluewite from Crestmore. No. 2. Waluewite from Slatoust, Urals. Analyzed by Nikolajef.5 No. 3. Waluewite from Slatoust, Urals. Analyzed by Clarke and Schneider.6 il 2 3 Si0, 16.74% 16.39% 16.85% UE KO Ro teeeeew. ae cue Al,O; 42.70 43.40 42.33 Fe.O, 2.85 1.57 2.35 FeO ‘ 041 0.10 0.20 CaO 13.09 13.04 13.30 MgO 20.03 20.38 20.77 Ign. 4.49 4.39 4.60 100.31 SRTETE 100.40 G—s.0sill Monticellite—The blue calcite contains monticellite in small masses and grains scattered through it in close association with the waluewite. One large specimen from the quarry consists of a wide band of massive monticellite separated from the blue calcite by a thin seam of walue- wite plates, while the calcite has individual grains and plates, respec- tively, of the two minerals. The color of the monticellite is flesh or pale brown and the luster is somewhat greasy. The irregular grains show cleavage faces, but no erystals occur. The mineral is practically infusible and is soluble in acids, forming a gelatinous mass when boiled almost to dryness. 5 Zeitschr. fiir Kryst., vol. 9, p. 579, 1885. Abstract. 6 Amer. Jour. Sci., vol. 43, p. 379, 1892. 1917] Hakle: Minerals Associated with Crystalline Inmestone — 343 Gordon Surr, analyst SiO, 36.02% 37.46% FeO 2.82 2.94 CaO 34.36 35.14 MgO 24.74 25.32 Ign. W325 2 sccaseese 99.19 100.86 GC 3:078 The occurrence of the monticellite and waluewite in close associa- tion is interesting because both have crystallized from the same silicate mixture and the waluewite may be viewed as having the composition of monticellite plus the spinel and alumina hydrate molecules. In the dis- cussion of the members of the clintonite group of silicates, Clarke and Schneider make the suggestion that waluewite may have the monti- cellite molecule in addition to its spinel and olivine molecules although no direct association of the two minerals was then known. Here we have the two crystallized together from a silicate mixture in which the monticellite molecule largely predominated and their erystallizations were practically simultaneous. The composition of the waluewite suggests a mineral mixture of monticellite + olivine + spinel + diaspore in an approximate ratio of 6:1:5:6. These monticellite and waluewite masses have in all probability been formed by the metamorphism of the brucite-limestone, while the common vesuvianite and diopside, which also occur in the blue calcite, but not associated with the monticellite and waluewite, are evidently products of metamorphism of the ordinary limestone, which has lttle magnesia. The former two were quite local in their development and were soon exhausted, while the latter are the abundant minerals of the quarry. Wilkeite—This interesting lime mineral with the four acid radicals has already been described,’ so only the essential parts of that deserip- tion will be given here. Boulders of blue calcite containing the granular pink wilkeite had just been blasted from the face of the quarry on the day the writer visited it, and fortunately specimens were collected of a mineral which would otherwise have gone unnoticed to the crusher. The wilkeite occurs as small grains and minute hexagonal prisms disseminated through the masses of blue ealcite. The mineral is clear 7 Amer. Jour. Sei., vol. 37, p. 262, 1914. 344 University of California Publications in Geology [Vou. 10 and glassy and usually pink but some grains are yellow. The mineral is essentially a calcium phosphate of the apatite group, with much of the phosphate replaced by the silicate, sulphate and carbonate mole- cules. A summary of the properties of the mineral are: Hexagonal system ; c= 0.730 approx. Prominent forms (1010) (1120) (1011) and (0001). Imperfect basal cleavage. H==5. G==5.234. Color pale pink or yellow. Luster vitreous or greasy. Optically uniaxial, negative. n= 1.640 + .005; n— n= .0004. Chemical composition is: SiO, 9.62% CaO 54.44 MnO 0.77 1240). 20.85 SO, 12.28 co, 2.10 HO — tr: 100.06 The formula derived from this analysis is: 3Ca;(PO,).-3Ca,SiO, . 3CaSO, . CaCO; . CaO. In order to better show its relation to apatite this may be written: 3Ca,(PO,)2- CaCO, + 3Ca, [ (Si0,) (SO,)] - CaO. During the past summer more of the wilkeite was observed in the quarry quite near the contact with the monzonite, in crystals several centimeters long, coated with its alteration product. This alteration substance coats the original grains and, in the absence of analyses, was thought to be okenite from its optical characters. There is a possibility that the delicate fibers optically tested are okenite; they cannot be separated from the intermixed wilkeite and their exact composition cannot therefore be determined. Much white secondary material has more recently been found which, as analyses show, does not have the ratio of lime to silica in the proper proportions for okenite. Since it is different from any known silicate, it is described below as a new mineral. Crestmoreite, a New Mineral.—Since the appearance of the paper on wilkeite, blue calcite has been found in the Commercial Rock quarry containing much soft white material disseminated through it in small bunches, as if it were an alteration, in place, of former crystals and grains included in the carbonate. Some of the blue calcite also contains large individuals of this white material having sharply 1917] Eakle: Minerals Associated with Crystalline Limestone 345 defined crystal boundaries, apparently hexagonal in outline. No wilkeite occurs in it, but it is evidently an altered product, presum- ably from wilkeite. Analyses show that it is principally a hydrous ealcium silicate with some of the silica replaced by the phosphate, sulphate and carbonate molecules. It is a new hydrous silicate of calcium having small amounts of the other oxides in place of the silica and the name crestmoreite, after the locality, is proposed for it. The mineral is compact snow-white with vitreous to dull lustre. H=3. G=2.22. It fuses quietly and easily to a shghtly vesicular glass. It is very easily soluble in acid, leaving some flocculent silica, while most of the silica goes into solution. Some of the lime can be extracted by boiling water. The earthy opaque material is not adapted to good optical deter- minations. It has parallel extinction, positive elongation, low bire- fringence and 6 = 1.590 + .005. Analyses of different samples of the mineral were made, all of them showing phosphates and sulphate in the substance. Some of the CO determined is due to calcite, which penetrates the mineral in thin seams SiO, 36.12% 38.30% 34.42% CaO 42.71 41.20 43.54 P30; 2.38 3.50 3.50 SO, 2.42 1.25 2.24 CO, E16 ee a 2 Ten. 14.98 15.17 16.24 EG 99.42 99.94 These analyses correspond approximately to the formula: 20H.CaSiO, . Ca,(PO,).. CaSO, . CaCO, + 101.0, and this requires the composition : SiO, 35.23% CaO 41.10 1P2 10}: 4.17 SO, 2.35 Co, 1.29 H.O 15.86 If crestmoreite were a clear crystallized mineral like the wilkeite, there would be no doubt that the phosphate, sulphate, and carbonate belonged to it and should be reckoned in its formula; but its earthy structure and composition show that it is changing to a ealeium silicate, and it is quite within reason to assume that the three acid radicals are small portions of those in the original wilkeite, which 346 University of California Publications in Geology [Vou. 10 have not been entirely leached out, in the hydration and silication of | the latter mineral, and therefore have no part in the formula for crest- moreite. An hydrous lime silicate is forming by the alteration of the wilkeite and the ratio of CaO: SiO, will be as 1: 1 no matter how much water, or in what way, it enters into the composition. Crestmoreite can be represented by the simple formula CaSiO,-H,O which requires SiO, 44.78% CaO 41.79 H,0O 13.43 This would make it a simple hydrous metasilicate like a hydrous wol- lastonite, but it seems more probable that crestmoreite, from the water determinations and derivation from wilkeite, is a hydrous basic ortho- silicate. The following percentages of water were given off at the respective temperatures : At 102° 1.25% 200 3.27 300 10.27 Red heat 15.11 Blast 16.76 In view of the fact that most of the water is expelled only at the higher temperatures it can be regarded as constitutional, and the above formula can be written H,CaSi0O,. Wilkeite is represented by the formula 3Ca,(PO,),-3Ca,Si0, - 3CaSO,-CaCO,-CaO, and it can readily be seen how the orthosilicate can increase at the expense of the more soluble phosphate and sulphate through the wilkeite alteration by carbonated and silicated waters. These waters were the heated ascending solutions which brought about some of the later crystallizations, and in the formation of the ortho- silicate part of the calcium was replaced by basic hydrogen. The exact formula for crestmoreite depends upon the water and therefore no formula can be advanced that is not open to eriticism. As a basic silicate most of the water must be considered as constitutional. The formula proposed for crestmoreite is 4H,CaSiO, +2H,0. This requires: SiO, 43.32% CaO 40.43 Constitutional H,O 12.99 ) Crystallization H,O0 3.26 i pte) 100.00 1917] Hakle: Minerals Associated with Crystalline Limestone 347 Riversideite, a New Mineral_—Some of the masses of vesuvianite contain narrow seams of a white fibrous mineral which has similar prop- erties to crestmoreite but with only half as much water, and it does not occur as an alteration of wilkeite, at least not as a direct alteration in situ. The mineral occurs in compact fibrous veinlets in the crevices of the massive vesuvianite and has a silky luster resembling satin spar. H=3. G=2.64. Fuses at 2 to a white glass. Easily soluble in dilute acid leaving flocculent silica. The mineral is a fibrous crystallization from the solutions carrying the altered wilkeite or crestmoreite and the analyses show that a lime silicaté with a ratio CaO: SiO, equal to 1:1 is, like crestmoreite, the principal constituent with small amounts of the phosphate and sul- phate present. In this case also the P,O, and SO, are hardly to be considered as belonging to the mineral. Analyses of the fibers gave: Mean SiO, 41.29% 41.22% 41.26% CaO 44.62 44.55 44.58 PZ O50) Te ee 3.84 3.84 SO, T8400) cecceest 1.84 HO 8.05 8.17 8.11 99.63 The water determination gave , At 102° 0.80% 150: 1.00 250 IBY Red heat CUTE Blast 8.05 This water analysis would indicate that it is mainly constitutional, but it is a difficult matter to construct a basic formula for the mineral that is satisfactory. The simplest. formula to express the composition of riversideite is 2CaSiO,-H,O. It may be likened to okenite with its basic hydrogen replaced by calcium: Okenite (H,Ca)8i,0, - H.0 Riversideite Ca, Si,O,-H.O The formula 2CaSiO,-H,O requires: si0, 48.00% CaO 44.80 HO 7.20 348 University of California Publications in Geology [Vou. 10 The analyses of riversideite correspond pretty closely to the formula 15H,CaSi0, - 15CaSi0, - CaSO,-Ca,(PO,), + 5H.0, which requires: SiO. 42.00% CaO 44.43 SO; 1:87 P.O; 3.31 HO 8.39 100.00 Disregarding the phosphate and sulphate it appears that the silicate formed is a combination of the basic orthosilicate and the metasilicate, and a formula to express the mineral may be written 6H,Ca,Si,0,-H,O. This requires : Si0, 47.43% CaO 44,27 Constitutional H.O 7.11 fl Crystallization H,O 1.19 § ce 100.00 The optical properties of riversideite kindly determined for the writer by Mr. E. 8. Larsen are: a=1,595 = 0,003, Parallel extinction. y= 1.603 + 0,003. Z parallel to fibers. The name riversideite, after the county in which it occurs, is proposed for this new hydrous lime silicate. The water content of a mineral is always subject to different inter- pretations; and it is not always possible to differentiate between hydroscopic, crystallization and constitutional water. Both of these new minerals might be interpreted as simple hydro-wollastonites. Crestmoreite CaSiO,-.H.O Riversideite 2CaSiO, . H.O Clinochlore—Small pale green flakes of clinochlore were found in the vesuvianite-masses at the Commercial Rock quarry. A patite-—Specimens of greenish blue apatite in granular form asso- ciated with green diopside and white wollastonite in white calcite were obtained from the quarry, but it does not appear to be an abundant mineral and no crystals of it have been collected. Aragonite-—Some of the hme carbonate has subsequently crystal- lized into the orthorhombie form. It occurs sparingly as fibrous and foliated thin layers interspersed with layers of quartz and calcite. 1917] Eakle: Minerals Associated with Crystalline Limestone 349 MINERALS ASSOCIATED WITH THE INTRUSIVES Feldspars.—Orthoclase, microcline, oligoclase, and labradorite are present in the quarries as constituents of the igneous rocks. Ortho- clase appears to predominate and it forms the larger part of the pegmatites. It occurs red and white. An analysis of the pure white from the pegmatites gave: SiO, 64.54% Al,O; 20.86 Fe.O, tr. CaO 1.86 MgO tr. Tgn. 0.52 Na.O ells K,0 11.85 100.81 Gra 54 Pyroxene.—Besides the good crystals of diopside which are scat- tered through the calcite, there is a deep green pyroxene resembling omphacite, mixed with cinnamon-garnet, which has formed at the contact of the pegmatite and lmestone. Augite-—Occurs as a constituent of the quartz-monzonite porphyry. Hornblende and Biotite—Both of these minerals are constituents of the granodiorite, the hornblende greatly predominating. Neither seems to occur in the monzonite or pegmatite. Titamte—Granular titanite is rather abundant in the monzonite as a constituent. It occurs pale brown with a marked pleochroism to deeper brown. None of the grains has a crystal boundary. Zircon.—Minute crystals and larger grains of zircon are scattered through some of the white pegmatite rock. The color of the mineral is clove-brown and some of the erystals show the forms (100), (110), (11), (331). Epidote-—Deep green epidote oceurs as one of the contact min- erals of the Commercial Rock quarry. Slender and long erystals and grains are imbedded in some of calcite masses. The mineral is very prominent as a constituent of the pegmatites and is one of the original minerals of the rock. It is present in the pegmatite as long slender erystals having a prominent basal cleavage. The fresh crystals are deep leek-green, but most of them have altered to a bronze-brown and resemble astrophyllte. The elongation of the crystals is parallel to 350 University of Califorma Publications in Geology [Vou. 10 the b-axis as usual, and they show striated domes with the cleavage base, but no end-faces. Quartz.—Specimens of compact granular quartz rock found in the talus of the Commercial Rock quarry indicate that seams of quartzite were formed in the crystallized limestone by its metamorphism. It is quite possible that sandstone seams occurred in the original formation and that these have been the source of much of the silica necessary to form such an abundance of silicate minerals. Quartz is a minor con- stituent of the igneous rocks and occurs in the usual smoky-brown color. Small druses of the mineral are occasionally found, but large crystals are rare. Tourmaline—Boron is a characteristic element in the rocks of Southern California and practically all of the pegmatites of that region carry boro-silicates, especially tourmaline. Three of these boro- silicates have been observed in the pegmatites of Sky Blue Hill and a few specimens have been collected, but the writer is without any data concerning them. The tourmaline is black columnar and occurs sporadic in the pegmatite. Axinite.—Violet-colored axinite associated with cinnamon-garnet occurs in large fragments in the pegmatite. Bright crystal faces, often striated, occur but erystals are not complete enough to measure. Axinite appears to be common in this particular region, as it is abundant at the Riverside quarry and has been noted in other places in the vicinity. Rogers® has described a large erystal from Riverside. Datolite—Glassy white datolite with shghtly greenish tinge occurs in connection with the pegmatites. The specimens sent to the writer are compact massive. Scapolite——Specimens of scapolite were recently collected by Childs. The mineral is in close association with green pyroxene, quartz, feldspar, wollastonite, and grossularite garnet. The color of the scapolite is grayish white, but it contains violet-blue streaks. The variety is probably wernerite. . Apophyllite—The masses of wollastonite which have formed on the contact between the pegmatites and lmestone contain cavities lined with small crystals of apophyllite. The erystals are colorless to white and are usually closely interlocked. Two habits are prominent; one is the common cubo-octahedral type with small faces of the pyramid and the base and second-order prism about equal in size. The other 8 School of Mines Quar., vol. 33, p. 373, 1912. 1917] Kakle: Minerals Associated with Crystalline Limestone Boll one is the pyramid type with a very small or no base. Only the three forms (001), (100), and (111) oceur on the crystals. Some of the erystals have been corroded by solutions and altered into white fibrous okenite. Okenite.—Radiating botryoidal coatings of okenite occur on the apophyllite evidently as an alteration product. The coatings consist of tufts of fibers and long slender needles. The acicular erystals are too slender for accurate measurements but they appear to be long prisms terminated on their ends by dull domes. Some approximate measurements and an analysis of the mineral were made by William Foshag. Measured (110):(1T0) 33°40" (010):(011) 52 00 (011):(0T1) 75 00 The analysis gave: Calculated for okenite H.Ca ( SiO, ) ».H20 SiO, 56.17% 56.60% CaO 26.10 26.42 H,O 16.83 16.98 99.10 100.00 The crystals have parallel extinction and are probably orthorhombic. H=44.5. G=2.206. Index of refraction 1.55. Low birefring- ence, 0.008-0.009. Solution in HCl yielding flaky silica. Fuses easily and gives water in a closed tube. It has formed from apophyllite through the action of carbonated waters, perhaps according to the equation : 2H,KCa,(Si0;), + H,CO; = 8H,Ca(SiO;), + K,CO3. Prehnite.—Two distinct varieties occur filling cavities in the white feldspar of the pegmatite. The first is the common green drusy prehnite. This is intimately associated with laumontite, which may be secondary from it. The second variety is unusual for prehnite. It is ght brown to colorless and lacks the drusy surface. In some of the cavities crystals line the walls, but they are so interlocked that single crystals are not separable. One erystal about five millimeters broad and one millimeter thick showed the forms c (001), m (110), a (100), and o (061). The base is large and bright but the edge-faces are dull. Most of this brown variety is compact granular with bright basal cleavage planes prominent. It is associated with massive datolite and gray quartz. 352 University of California Publications in Geology [Vou. 10 An analysis of this brown variety gave: Si0, 44.10% Al,O; 24.20 CaO 25.20 H.O 5.86 99.36 Laumontite-—The green prehnite has laumontite coating it in small divergent columnar and fibrous masses. It has the appearance of a secondary alteration of the prehnite and in all probability it is such, although there is no direct evidence to prove it. The mineral is snow- white with vitreous luster. Some of the stouter needles have the characteristic oblique cleavage ends. It fuses readily to a vesicular glass and is easily and completely soluble in HCl, yielding a thick gelatinous mass. An analysis gave : SiO, 53.49% Al,O, 22.01 CaO 10.80 MgO tr. H,O 13.39 99.69 Opal.—White hyalite coats the walls of some of the cavities in the feldspathic pegmatite, and it coats the apophyllite and okenite to some extent. Under the electric spark it shows strong yellow luminescence, which is an indication that it contains uranium. The amount of material on hand is too small to determine the uranium chemically. Besides this hyalite opal there is considerable wood opal in some portions of Sky Blue Hill. It is dark brown and black, becoming gray by heating. It shows the wood structure and some of it has small calcite rhombohedrons deposited on it. SULPHIDE MINERALS Arsenopyrite, pyrite, galena, sphalerite, greenockite, bornite, chaleopyrite, and tetrahedrite occur in the Commercial Rock quarry, mostly in association with the pegmatite intrusives. Arsenopyrite has been found in a few small crystals about two millimeters long. Pyrite is more disseminated than the other sulphides. It occurs in grains, cubes and pyritohedrons, and much of it is altered into brown limonite pseudomorphs. 1917] Kakle: Minerals Associated with Crystalline Limestone 353 Galena occurs in rather large cubes and also massive granular. The specimens collected are associated with garnet dodecahedrons, quartz, sphalerite, pyrite, and chalcopyrite. Sphalerite is quite black but has the characteristic resinous luster and good cleavage. It occurs in the vesuvianite-garnet masses and some of it contains small coatings of bright yellow greenockite. The copper minerals, bornite, chalcopyrite, tetrahedrite, and per- haps chaleocite, have been found in grains and small granular masses in the metamorphic zones of silicates. OXYDATION PRODUCTS Azurite and malachite occur as thin coatings and as stains in the vesuvianite-garnet mass of rock. Cerussite and anglesite have both been identified as earthy gray coatings on the galena. The two oxides of iron, limonite and hematite, are common in small earthy masses and as stains. The weathered brucite limestone of the Commercial Rock quarry has much yellow earthy limonite and deep red hematite filling the cellular cavities left by the leached-out brucite. The crystals and grains of pyrite imbedded in the calcite and even in the pyroxene and other silicates have been largely altered into lmonite pseudomorphs, probably readily changed by the action of the carbonated waters. White clay from the orthoclase and chlorite from the epidote, augite, hornblende, and other silicates are natural alteration products. PLATE 21 View looking northeast, showing the two hills and the cement plant of the Riverside Portland Cement Company at Crestmore, Riverside County, California. The quarry floor marks the juncture of the limestone and granodiorite. [354] UNIV GAEE sPUBES BUELS DEPT. (GEOL [EAKLE] VOL. 10, PL. 2 PLATE 22 Three views showing different portions of the commercial rock quarry on the eastern side of Sky Blue Hill. The quarry face and boulders are mostly mixtures of blue and white calcite, brown vesuvianite and garnet and green diopside. [356] UNIV CARI. “PUBEM BUELL DEPT. GEOE. [EAKLE] VOL. 10, PL. 22 Siw ies PLATE 23 Projections of wollastonite erystals, showing the different types and com- binations of forms. Figure 1 is the type most common for wollastonite. Figures 2 and 3 are types common at Crestmore. The left half of figure 3 is the rear of the right half drawn to show a center of symmetry only, if the crystal were doubly terminated. Figures 4 and 5 are orthographic projections of the ends, showing better the front and rear faces and the absence of an axis of symmetry. [358] UNIVICALIES PUBE BUEE, DEPT. GEOL. (EAKLE] VOL, 10, PL. 23 SS PLATE 24 Figures 6-8 are projections of vesuvianite erystals showing the general type, but different combinations of forms. Figures 9 and 10 are diopside, showing the characteristic type and combinations. [360] oe 2, pls. 2 GEOLOGY AND ORE DEPOSITS OF _THE LEONA RHYOLITE BY - - CLIFTON W. CLARK UNIVERSITY OF CALIFORNIA PRESS BERKELEY UNIVERSITY OP CALIFORNIA PUBLICATIONS oe Nore.—The University of California Publications are offered in exchange for t th eations of learned societies and institutions, universities and libraries. Oo all the publications of the University will be sent upon request. For sample cop publications and other information, address the Manager of the University Pres’ California, U. S. A. All matter sent in exchange should be addressed to The Department, University Library, Berkeley, California, U. S. A. y Orro HaRRASSOWITZ R. FRIEDLAENDER & Sonn 7 LEIPZIG . BERLIN Agent for_ the series in American Arch- ‘Agent for tke series in American : acuiogy anu wuinuiugy, Classical Philology, aeology and Ethnology, Agricultural Sciences, Keonomies, Education, History, Modern Botany, Geology, Mathematics, Pathology, Philology, Philosophy, Psychology. Physiology, Zoology, and Memoirs. Geology.—ANDREW C. Lawson and JouN C. Merriam, Editors. Price, volumes 1-7, $ volumes 8 and following, $5.00. ; b: Cited as Univ. Calif. Publ. Bull. Dept. Geol. Volume 1, 1893-1896, 435 pp., with 18 plates, price .0..c.-.cc.ccccccseeeteecesenene ieee 3.50 Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price -...2...c-cs-ccececeee---e-e av: Volume 3, 1902-1904, 482 pp., with 51 plates, Price. .2..22s.22.-ceccsecceecteeceerseseebeeee oe Volume 4, 1905-1906, 478 pp., with 51 plates, price <..2:-.2c.2.-ccscccecccecseeeceteeceenencereoeee Volume 5, 1906-1910, 458 pp., with 42 plates, price 2-.25-2. 32 eee A list of titles in volumes 1 to 5 will be sent upon request. VOLUME 6. “S 1. The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller................-.... 2. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern Nevada, by John C. Merriam. Part [.—Geologie History............-----teccececseceeeseeeceene 3. The Geology of the Sargent Oil Field, by William F. Jones 4, Additions to the Avifauna of the Pleistocene Deposits at Fossil Lake, Oregon, by ea Lioye Holmes, Miller ~-_.o0c2c...3. 2:35. 3 eccectnn-tente: soe -}omenerate ete nondtnengtenee sie be . The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Reid 60e . Note on a Gigantie Bear from the Pleistocene of Rancho La Brea, by John Cc. Merriam. . A Collection of Mammalian Remains from Tertiary Beds on the Mohave Desert, by John C. Merriam. Nos. 6 and -7 Im one COVER «.:.--2..28..s-cbgced see cceencnn sstesttapaene-seeet) ae rr 8. The Stratigraphic and Faunal Relations of the Martinez Formation to the Chico ; and Tejon North of Mount Diablo, by Roy HE. Dickerson ......- ieee ; 9. Neocolemanite, a Variety of Colemanite, and Howlite from Lang, Los Angeles” is County, California, by Arthur S. Bakle {shoehorn 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. Taylor... — 11. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern ’ NI ao Nevada, by John C. Merriam. Part Il.—Vertebrate Faunas ...0.. 222222. ecceeeseeeeeeees 12. A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, by Loye Holmes MU er oon ecsccasaa dic oneene MR tbesb edb ec non tdeces Lana: Pavegsae! eet nae ee, Seas tay ei cen Oke rr 13. Notes on the Relationships of the Marine Saurian Fauna Deseribed from the Triassic » of Spitzbergen by Wiman, by John C. Merriam. 14. Notes on the Dentition of Omphalosaurus, by John C. Merriam ard Harold C. Bryant. Nos. 13 and 14 in one) Cover 2.2. S2256.2. 2S. ge ee eo ; 15. Notes on the Later Cenozoic History of the Mohave Desert Region in Seutlleschaedt om California, by Gharles Laurence, Baker (2 cnc sccoccct. tose nne eet nc ed oe enn 16. Avifauna of the Pleistocene Cave Deposits of California, by Loye Holmes Miller .. per 17. A Fossil Beaver from the Kettleman Hills, California, by Louise Kellogg. Bee f 18. Notes on the Genus Desmostylus of Marsh, by John CO. Merriam occ 19. The Elastic-Rebound: Theory of Earthquakes, by Harry Fielding Reid ~.............-.- VOLUME 7. 1. The Minerals of Tonopah, Nevada, by Arthur S. Eakle 2. Pseudostratification in Santa Barbara County, California, by George Davis hoader: WS Chee wet se scien eens come eae ae act ee cae ee ee 3. Recent Discoveries of Carnivora in the Pleistocene of Rancho La Brea, a tae IMO Tri’ osc cies Be se one nc cee aan a OE ea is sr L. Clark ven ca dee é UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 20, pp. 361-382, pls. 25-27, 3 text-figures November 8, 1917 THE GEOLOGY AND ORE DEPOSITS OF THE LEONA RHYOLITE BY CLIFTON W. CLARK CONTENTS PAGE Character and Purpose of the Work ........2..2..2.2-.2:22:2::21:2ceceeceeceeceseceeeeteeeeeeeeeeeeeeeees 362 Physical Features of the Area, .-.....-.-----sc-cccccecce-ceceecececdecceceeceecencescesectneteessceasssenccee 862 He VE CEM be WTOSVONAN SULLAC EC. ecceccceccesce2eceetecenzeecocce sense cece cceeea-ccseecacceareeceeeerarecseee 363 Greolo mice MEla St 0 rayaeee ees tear oe eect eae So ee eee ee ca ndaettenadecuns 364 Mistmibmtvon: Of the ENG OUtE <...clccescie.oectcenetaccccccnsececsseceecenneectetesteeasse voveiex Seas 365 Nature of Surface upon which Lava Flowed .............22.22..2..2..2-.2-2---0200-0000eeeseo-o 365 ENCE OBE EOE. VE Sy 00 I ee eS ee aa eee 366 PEPER UH LIN pee msce ests ce SNe aso eee ec ce ae eae ee ae a cee sah cape ees Ssek cacacunceceysencsabeadeatpecksens antes iciesns 366 General Features of the Rhyolite -..............22.220.22..22-.2ce-ceeceeeceeecneeeeeeeeeeeeeeeeeeeeee B67 Neetmoonap ur Cal CHaracteEs assrs..cec:2essecetescsce ss tose veeetasctteec dees hen seceetotas¥bseatesancsecesdete-stetcs 368 IHC SUC CME ACT OS) eecct cst sees see eae ae een cet 8 ee eee epee een ose cent et nce 368 TNE Oy 6) 5 AATCC GNSS ee 369 RY Air lavy sla CE eC Cg Meenas ee sense ew Se eed se nes oases eee oe Se a Sette eeea canes 369 Marcrolatie. NaCles: see .8 ss 25- ie ees cece, ee eee ee 369 Distribution of the Different Facies ..............2-..---2-..22.22:e-1ceeeeeee ee ece eee 370 Summary of the Microscopic Study -22.2..csccccc. cc acc cena cece eect ete eens Byal Oe mic aC hana Chers: see vies csrec cee ccc -careccsaylersst2scsnsdvencee socessbexseecerstsetieccedetertcct sdcstecesocaateh 371 TES aeri ee) SUE OX oF are eee ee Ee 372 NU Ct LO YIN] ease see eee ces eco Ps acse cscs See s2sdztnseadidosSsnceseceaec tet casa¥eecatectsiezdsestees 372 \Ofraoleornpemrrawiin | IDYeNiq ea a woK eva es a eee 373 CCUM CTAC ares ere ee mie ee Bc sae esas eg See oat Si cnete coe eects sete tet. STs seen eda 373 MVAbiie rea O eye peeeeetate ens ee ecw pens ceeccs sve cethenccedessicts sense escaeeedsaccaestesdesd-icedeeeieszeeesesetsateec 374 WilcoueaUoyeiean oboe TShiuus bye (one lek (ON eh eee a ee 374 (Ch cemmucess iss OIE NS COREY are re 375 The Relation of Fracturing to the Ore Deposit --...------------------------------ 377 The Reducing Effect of the Rhyolite —....-...-.------------------ceecseneeeeeeeeececeeceeeees 377 SWINTON cates eter eS se ee CS Pe 379 362 University of California Publications in Geology [Vou. 10 CHARACTER AND PURPOSE OF THE WORK During the fall of 1915 and part of the winter of the year 1916 the writer spent considerable time in the study of the Leona rhyolite as to its extent, its petrographical character, the nature of the surface on which it rests, its structural features, its age and the ore deposits 1m it. Professor A. C. Lawson’ in the San Francisco Folio has given a brief account of the rhyolite and its relations and mapped its distri- bution. He also devotes a paragraph to the description of the ore deposits. It is the purpose of this paper to give a more detailed description of this very interesting feature of Coast Range geology.” PHYSICAL FEATURES OF THE AREA The area occupied by the Leona rhyolite is confined to a portion of the front of the Berkeley Hills, which form the steep northeast boundary of the valley of San Francisco Bay. The cities of Berkeley and Oakland are in part located on the foothill slopes, but for the most part they are situated on the alluvial embankments, in part terraced, at the base of the hills. These embankments are now being dissected by the streams which formed them. The front of the hills has a straight northwest-southeast trend and is continuous in its abrupt elevation above the bay plain from San Pablo to the town of Hay- wards, except for a few canons which dissect it. A remarkable break, however, oceurs at Haywards, where Castro Valley forms a flask- shaped embayment connecting by a narrow gap with the Valley of San Francisco Bay. The rhyolite, being more resistant to erosion than the surrounding formations, stands out in relief along the front of the hills from its northern end at Berkeley to the vicinity of Haywards. But south of this point it is less prominent and conforms more to the aspect of the topography of the adjacent rocks. The rhyolite is everywhere studded with erystals of pyrite, the oxidation of which has given the characteristic reddish color to the formation. In certain sections where the outcrop of the rhyolite is obscure, the color of the soil derived from it was of material aid in determining its boundary. 1U.S. Geol. Surv., San Francisco Folio, no. 193, 1914. 2The writer wishes to express his thanks to Professor A. C. Lawson for helpful suggestions and criticism in the preparation of this report, and also to Mr. D. A. McDonell, General Manager of the Leona Chemical Mine, and to Mr. J. M. Conlin, Mine Superintendent, for many courtesies extended during the examination of the mine. 1917} Clark: Geology and Ore Deposits of the Leona Rhyolite 3638 Pre-Recent Erosional Surface.—In the vicinity of Elmhurst there is evidence of an old erosional surface whose remnants form part of the present topographical surface. The general direction and possible extent of the stream which flowed on this surface is shown by the sketch map in figure 1. It is not known how extensive this former surface may have been, but the evidence used in making the map consists of the presence of stream pebbles composed mostly of Oakland conglomerate and boulders of Chico sandstone. The pebbles found lying loose upon the surface are probably the last trace of the former stream deposits. The small area north of Lake Chabot, mapped as Knoxville, is partially occupied by these pebbles imbedded in alluvium Fig. 1. Sketch, in part, hypothetically drawn, showing the pre-recent stream system and its relation to the present topography. The dotted lines represent the pre-recent stream valleys. The branching full lines represent the present streams. The heavy lines represent faults. derived from the formations to the east. North of the F. C. Talbot ranch about a mile, along the road leading to the country elub, there is a considerable thickness of the old river gravels. Here cross- bedding is well exposed on both’ sides of the former stream valley. To the south of the road just referred to, in an old stone quarry, the stream gravels are exposed in vertical section. The deposit is about ten feet thick and rests on an uneven eroded surface of the rhyolite. This old stream valley has a course transverse to the present streams. The presence of pebbles on the tops of some of the hills indicates that the former stream system antedates that of the present by a considerable period of geologic time. The direction of the present stream valleys being at such variance with those of the pre-Recent indicates that the former were superim- 364 University of California Publications in Geology (Vou. 10 posed upon the latter. A considerable portion of the country just east of the Haywards fault was covered with detritus and then elevated, the uplift giving rise to the present stream system. As near as can be judged, at least a branch of the old stream flowed out through Arroyo Viejo Creek during the last stages of its existence. There must have been a large amount of detrital material deposited on the lower hillslopes at the advent of the present erosional cycle. This material has been largely if not all covered by recent alluvium. The former stream system probably represents the period in which the San Antonio formation was deposited. Material similar to that in the San Antonio formation covers a considerable area of the Knox- ville just north of Lake Chabot. The material here, however, contains many large boulders, which at some places are imbedded in the finer alluvium; it is the finer alluvium that is similar to the San Antonio. GEOLOGICAL HISTORY The portion of the Berkeley Hills here considered is composed of several kinds of rocks, both igneous and sedimentary. The oldest of these, comprising sandstone, conglomerate, quartzite, radiolarian chert, serpentenized peridotite, diabase, ellipsoidal basalt, and glaucophane schist, compose the Franciscan group. Upon this group the lower Cretaceous or Knoxville formation rests unconformably. It is pre- vailingly a fine-grained arenaceous and carbonaceous shale having a thickness of several hundred feet. As has been pointed out,* the shale contains no coarse sand or conglomerate at its base, which would signify a slowly transgressing sea. The lack of this coarse material would seem to indicate that the surface of the Franciscan must have been reduced to low relief and submerged rapidly. Upon the Knoxville shale rests the Chico or upper Cretaceous. The Oakland conglomerate at the base of the Chico ranges in thickness from 100 feet near Temescal Lake to perhaps 800 or 900 feet east of Leona Heights; near Lake Chabot it reaches a thickness of 1000 to 1200 feet; but it is probably not thicker than 1000 feet near the southern end of the Haywards quadrangle. The upper portion of the Chico is composed of sandstone and shale many thousand feet thick. The apparent conformity of the Oakland conglomerate and the Knoxville is an interesting point connected with the geologic history 3 Op. cit., p. 4. 4 Op. cit., p. 8. 1917] Clark: Geology and Ore Deposits of the Leona Rhyolite 365 of the region which is discussed in the text of the San Francisco Folio. The pebbles of the conglomerate are mostly chert, shale, and sandstone, but along with these are numerous boulders of granite and grano- diorite. It seems, therefore, that there must have been marked dia- strophic movements at the close of the Knoxville epoch, but these movements were not of such a nature as to raise the Knoxville sedi- ments above sea-level. After erosion which locally removed the Shasta-Chico rocks, the Leona rhyolite was extruded on the surface as a lava flow. From its present disposition it appears that the flow probably followed an ero- sional valley. The valley must have roughly followed the contact of the Knoxville and the Franciscan. Since the extrusion of the rhyolite there have been several crustal movements.® These movements have continued up to recent geologic time, as is shown by the various alluvial deposits, and also by the present streams that in many instances show recent readjustment. The most recent movement has been faulting along a line generally parallel to the Berkeley Hills. DISTRIBUTION OF THE RHYOLITE The rhyolite forms a narrow discontinuous belt that extends from Hamilton gulch at Berkeley to a point about five miles southeast of the town of Haywards, a total length of about twenty-two miles. The lava flow has a maximum residual thickness of about 400 to 600 feet, but generally it is much thinner. It presents a rather distinet physio- graphic feature on the front of the hills due to the steep slopes of its erosional forms. At a number of localities the streams have eroded through the entire thickness of the rhyolite and are now cutting into the older rocks below. Indeed, it seems quite evident that the dis- continuous areas of rhyolite are remnants of a former continuous lava flow that was much thicker and wider. NATURE OF SURFACE UPON WHICH LAVA FLOWED In some places the rhyolite rests upon the Franciscan, in others upon isolated patches of Knoxville which were not entirely removed from the Franciscan by erosion at the time of its extrusion, so that the lava probably occupied the valley into which it flowed.. It was hoped that considerable quantities of stream gravel would be found below 5 Op. cit., p. 20. 366 Umversity of California Publications in Geology [Vou. 10 the rhyolite, but in two or three places only were any gravels found in such a position, and in these places in very limited amounts. How- ever, this does not preclude the possibility that they underlie the rhyolite, because in only a few places is the base of the rhyolite clearly exposed. The field relations and petrographical character of the rhyolite, which will be discussed later, indicate that the lava probably came from one source and was extruded as a single flow. AGE OF RHYOLITE The age of the rhyolite is one of the principal points to be consid- ered, but after much detailed study of its relation to the adjoining formations the time of extrusion has not been narrowly determined. It is certainly post-Chico, and, judging from the degradation of the surface upon which the rhyolite rests, the degree of its alteration, the amount of its erosion, and the extent of post-rhyolite movements, it seems highly probable that it is as old as Pliocene, as has been suggested.® FAULTING The Berkeley Hills orogenic block’ is a feature of especial interest in the geology of the Coast Ranges in the San Francisco Bay region. The Haywards fault, which traverses this region nearly parallel to the trend of the rhyolite belt, is comparable to the San Andreas fault because of the similar geomorphic features it has produced. It ex- tends through the area mapped, from Berkeley southeast along the base of the steep slope to the vicinity of Temescal Lake, where it be- comes manifest as a rift valley to a point southeast of Leona Heights ; here it turns in a more southerly direction and passes through the low front ridge of the hills out under the alluvium. At Arroyo Viejo Creek the rift again returns to the rhyolite area and passing up this ereek in a southeasterly direction through a well defined saddle on the F. C. Talbot ranch connects with the oblique fault west of Lake Chabot. The main fault may be offset somewhat by this oblique fault, but from this point it has been tentatively drawn on the map through the several saddles and breaks in the western slope of the hills to the town of Haywards, where it is lost as it passes out under the alluvium. 6 Op. cit., p. 12. 7 Op. cit., p. 17. 1917] Clark: Geology and Ore Deposits of the Leona Rhyolite 367 Numerous faults of smaller dimensions and probably intimately associ- ated with the Haywards fault have been observed in the area. These minor faults are oblique, parallel, and transverse to the Haywards fault. The northern exposure of rhyolite is cut off at Hamilton gulch by a fault that is transverse to the major movement. This portion of the rhyolite is also faulted against the Chico and Knoxville formations along most of its eastern boundary. At Leona Heights two faults more or less parallel to the Haywards fault and undetermined in extent have aided in producing the geomorphic features of this locality. South of Lake Chabot and again south of Haywards oblique faults extend in a southeasterly direction from the main fault. These ob- lique faults are probably connected with a main fault, approximately parallel to the Haywards fault, that traverses the country from Lake Chabot southeasterly. In general the relative movement along the fault plane appears to have been horizontal rather than vertical. At Temeseal Lake quite extensive masses of gouge and breccia are exposed at the surface in a railroad cut that traverses the fault for a short distance. It does not seem likely that this amount of gouge was produced by any vertical movement that could have taken place here. It is quite certain that a considerable movement has occurred along the Haywards fault in recent geological time, as is evidenced by the diversion in the direction of the streams that flow transverse to the fault valley. Any statement as to what effect the faulting has had in the geomorphogeny of the region, the number of movements and the geologic epoch in which they occurred would be largely conjectural. But there probably have been several periods of movement along this fault zone in post-rhyolite time, and there is a possibility that the rhyolite may have been extruded at some point on the zone. GENERAL FEATURES OF THE RHYOLITE The Leona rhyolite reaches its maximum width of one and one-half miles a little north of the F. C. Talbot ranch, east of Elmhurst. The lava varies in thickness, but reaches a maximum of perhaps 600 feet. Where fresh the rhyolite is hght green to bluish in color and varies in texture, being glassy and porphyritie in the northern part, while towards the southern end it is less porphyritic and becomes more felsitic. The rhyolite is everywhere studded with pyrite erystals and contains very few ferromagnesian minerals in the fresh rock. Certain 368 University of California Publications in Geology [Vou. 10 facies show amygdaloidal structure, but flow structure is not common, except in certain glassy facies. It is everywhere jointed and frac- tured and under weathering processes yields a soil which contains numerous angular fragments. The chemical alteration of the pyrite has produced iron oxide that stains the soil to a characteristic brown or red color, so that the regolith of the lava is readily recognized in the field. PETROGRAPHICAL CHARACTERS The Leona rhyolite may be divided into four facies, according to texture. The first, which shows the most advanced degree of crystal- lization, has a felsitic texture and is composed of quartz and feldspar, which only rarely attain phenocrystie development. This will be known as the felsite facies. The second facies is similar to the above, but consists of pheno- erysts of feldspar and quartz set in a dense groundmass that in places is microcryptocrystalline, but is generally eryptocrystalline. This will be designated the felsophyric facies. The third facies is characterized by well developed quartz and acid plagioclase phenocrysts set in a glassy ground mass and will be desig- nated the vitrophyriec facies. The fourth, or microlitic facies, may well be divided into two varieties, one the glassy and the other the spherulitic. The glassy variety has a hypoerystalline ground mass which grades into a dense glass. The erystalline constituents of the ground mass are mostly quartz, but minute needles of feldspar are sparingly included in the matrix. The spherulitic variety has a glassy ground mass which shows radiolitie areas as distinct from the more dense glass. This grades into devitrified areas which show a eryptocrystalline character. The spherulites are sporadically distributed through the matrix, and also oceur sparingly embedded in the phenocrysts. Felsite Facies —This is a brownish white rock, composed of feld- spar and quartz, having a subeconchoidal fracture and a felsitic texture. A very few phenoerysts of oligoclase are present in the ground mass, which is eryptocrystalline and altered. The quartz crystals are fre- quently rounded by corrosion, but in spots secondary quartz is present in quite large aggregates along fractures. The accessory minerals are pyrite, magnetite, leucoxene, and small needles of apatite. 1917] Clark: Geology and Ore Deposits of the Leona Rhyolite 369 Felsophyric Facies.—This is a light green to brown rock contain- ing numerous dense, cloudy, indistinct patches. It has a subecon- choidal fracture very similar to that of the rock just described. The ground mass is composed of feldspar and quartz in various irregular aggregates. The white clouded patches appear to be composed of alteration products which are not determinable. In the finer part of the matrix chlorite is present, producing a bluish-green stain in the altered products. The phenocrysts are mostly plagioclase, but a few aggregates of orthoclase and quartz occur in the matrix. The acces- sory minerals are pyrite, magnetite, zircon, and apatite. Vitrophyric Facies—This is a hght blue to gray rock having a eryptoerystalline ground mass which appears under the microscope to grade into a hypocrystalline aggregate. Numerous crystals of feld- spar, together with some quartz and irregular masses of magnetite, constitute the phenocrysts. A few flakes of biotite partially altered to chlorite are also present in the rock. The small aggregates which make up the matrix are of two kinds: one is principally composed of rounded grains with rare elongated forms, while in the other the elongated crystals of feldspar and quartz form most of the ground- mass and the few rounded grains present have been derived mostly by alteration and addition of secondary quartz. The phenoerysts are mostly oligoclase feldspar and quartz, with a few poorly developed erystals of orthoclase. Some of the feldspar phenocrysts have been partially silicified, so that they appear as a dense brownish colored mass that does not always show the original erystalline structure. The accessory minerals are pyrite, magnetite, apatite, and zircon. Microlitic Facies.—The microlitie facies is composed of two varie- ties of glassy rock. 1. The first has a eryptoerystalline ground mass which grades into an undeterminable, brownish glass studded with minute elongated feld- spars and grains of quartz. In portions of the rock these elongated needles of feldspar are oriented in a single direction, giving rise to a flow structure which is common in this facies of the rhyolite. Feld- spar forms the most important phenoerysts, if we exclude certain quite large aggregates of quartz and irregular masses of magnetite in the matrix. Most of the feldspar is altered to kaolin and silica, which form dense clay masses colored dark blue by chlorite. Certain portions of the rock frequently show an intermediate stage between the dense glassy base and the microlitie structure. 370 University of California Publications in Geology [Vou. 10 2. The second variety is of a light gray, green or bluish color, except where stained with iron oxide; it has a subeonchoidal fracture, appears massive, and is very hard. Under the microscope the ground mass appears to be cryptocrystalline or microlitic, and in it are scat- tered numerous groups or aggregates of spherulites, which are of two kinds: those that are in circular groups imbedded in a dense brown glass, and those that are sporadically scattered through the ground mass, and are also present in the altered phenocrysts. The former are microscopic in size, spherical in shape and show no distinct radiating fibers, but give a black cross between the crossed nicols, as shown in plate 25, figure A. According to Iddings,* the number of plates of feldspar composing such spherultes increases to such an extent that the outline of each individual plate is lost; and when no distinet trace of any single fiber can be seen the ideal spherulite is produced. The second kind of spherulite is composed of fibers and plates, whose out- lines can be seen under the microscope. In some eases they appear to radiate from a small grain at the center, probably quartz. These spherulites do not show a black cross between the crossed nicols. They appear to be as numerous in the altered phenocrysts as in the glassy matrix. According to Iddings,® spherultes of this type are composed of radiating plates or prismoid crystals. An example is shown in plate 25, figure B. This variety of the microlitic facies does not show the flow lines as distinetly as that first described, but both kinds of spheru- lites are present in most of the sections examined of this facies. DISTRIBUTION OF THE DIFFERENT FACTES The four types of rhyolite have a rather definite distribution along the extent of the outerop. The rock grades from a more glassy facies at the northern end of the belt to a more crystalline facies at the south- ern end. Both varieties of the glassy facies were obtained in that por- tion of the belt between Berkeley and Leona Heights. At Leona Heights some of the specimens collected were glassy, while others showed a distinet porphyritic character. From the vicinity of Leona Heights to Lake Chabot the rock is predominately porphyritic in text- ure. South of Lake Chabot to the town of Haywards the felsophyric facies predominates; that is, the ground mass in the rhyolite becomes much more granular and the glassy material is not so common in the 8 Iddings, J. P., Igneous Rocks, vol. 1, p. 229, 1909. 9 Op. cit., p. 229. 1917] Clark: Geology and Ore Deposits of the Leona Rhyolite 371 matrix. In this facies the phenocrysts are much less common, and those present are of small dimension. The rhyolite southeast of Haywards has been classed as felsite. In this portion of the outcrop alteration has been so intense that fresh rock is very hard to obtain. However, the rock shows a rather uniform felsitie texture, with a feeble development of small phenocrysts. SUMMARY OF THE MICROSCOPIC STUDY The petrographical study of the rhyolite shows that it may be divided into four facies largely based upon textural differences. The series includes a range of facies from those which are mostly glassy to those which are holocrystalline containing only a few small pheno- erysts. The rock is comparatively simple and rather uniform in compo- sition. Orthoclase, plagioclase, mostly oligoclase, and quartz are the essential constituents of the original rock. The accessory minerals are pyrite, magnetite, apatite, zircon, and leucoxene. Only the first three mentioned are in abundance. This study seems to support field evidence that the different facies are probably products of a single lava flow and came from a common source. CHEMICAL CHARACTERS The chemical composition as given in three different analyses is as follows :1° (Ca ee) ee Trace ee Vet{O) (enn OO)? (Op) ere, .28 06 .07 Ueda re eee eee eee 1.56 .96 55 100.37 =99.96 100.21 (1) Analyzed by C. P. Richmond in the laboratory at the University of California. (2) and (3) Analyzed by G. E. Colby in the laboratory at the University of California. 10 U. 8. Geol. Survey., San Francisco Folio, no. 193, p. 12, 1914. 312 Uniwersity of California Publications in Geology (Vou. 10 The analyses cannot be considered to represent the composition of the original rock, for all of the specimens collected have suffered partial alteration. The high content of silica and low percentage of lime, with a rather high content of Na to that of K, indicates that the rock is a soda rhyolite. The rather constant percentage of Al,O, in the three analyses given above is of interest because in all the sections studied of this rock free kaolin was observed as an alteration product. N O 100 200 Feet eco oe EE | Fig. 2. Plan of mine workings. PYRITE DEPOSIT Location.—Near Leona Heights, east of Oakland, deposits of pyrite occur in the rhyolite which have been mined for a number of years. At the present time two mines are in operation, one having just re- cently started. One of these mines, once known as the Leona Heights Mine, was described in 1911.1. The larger mine, operated by the Leona Chemical Company, is the principal source of information con- tained in this report. 11 Mace, Clement H., Min. and Eng. World, vol. 35, p. 1320, 1911. 1917] Clark: Geology and Ore Deposits of the Leona Rhyolite 373 Underground Development.—The mine of the Leona Chemical Company is opened by two tunnels entering the hill at two levels, 75 feet apart. The approximate position of the tunnels and of the ore body is shown in figures 2 and 3. The ore observed in the workings is in a potato-shaped mass in the mineralized zone, and is of two kinds. The soft ore is nearly everywhere surrounded by gouge ranging from a few inches to two or three feet in thickness. The hard ore, which forms but a small part of the deposit, is highly silicified, contains more chaleopyrite, and is not bounded by fault gouge. Most of the ore has been taken from the lower level, although quite important bodies extend above the upper tunnel. A winze was put down 40 feet from the north crosseut on the lower level, and it is said oO 50 190Feet 100 Ft Level WSS SSSI NX Ft SQAQAQ SS KN SEAS “ MAA SOX ORNS Fig. 3. Diagrammatic vertical section of ore body along line A—A’. that ore was encountered all the way down. A raise was driven from the southeast part of the lower tunnel and ore was struck 20 feet above the level, so that it is evident that the ore body dips into the hill, as is shown in the vertical section. Occurrence.—The ore is confined to the rhyolite and is not in contact with any other rocks so far as is known, but the deposit described by Mace’? rests on a shale, probably Knoxville, and not a part of the Franciscan, as he suggests. The pyrite is massive and has fragments of country rock included in it. The ore occurs in a fracture zone in the rhyolite, which is jointed and faulted so that considerable quantities of gouge and small displacements may be seen nearly every- where in the mine; but there is abundant evidence of more intense fracturing and differential movement that has probably caused the localization of the ore bodies. At nearly every place in the mine where the margin of the ore is 12 Op. cit., p. 1320. 374 Unwersity of Californa Publications in Geology [Vou. 10 exposed the latter is surrounded by a considerable thickness of gouge composed mostly of kaolin and silica partly replaced by pyrite, an illustration of which is shown in plate 26, figure A. The pyrite com- monly grades out from the solid ore through the gouge into the wall rock. In some of the most recent workings a hard type of pyrite has been encountered. Although a small mass of this was struck on the lower level, yet the main body was encountered in a raise from this level. This ore contains a considerable quantity of chaleopyrite. The wall rock adjacent to the ore, and into which it grades, is highly silici- fied and contains small masses of kaolin. It is more thoroughly erystal- hne, contains a larger percentage of silica, and is much harder than the other type of pyrite. An illustration of this is shown in plate 26, figure B. Mineralogy—The minerals derived from the ore according to Schaller'® are pyrite, chalcopyrite, copper, melanterite, pisanite, chal- canthite, copiapite, epsomite, hematite, limonite, alunogen (?) and boothite. Besides these the writer has observed chalcocite, bornite, and sphalerite in the ore. The pyrite, however, is the only mineral of economic importance and is used to make sulphuric aeid. Metallographic Study of the Ore-——A number of polished surfaces of the pyrite and of the country rock partially altered to pyrite were studied for the purpose of determining the nature of the metasomatic replacement of the rock by the pyrite and associated sulphides. The two types of pyrite already described show a rather marked difference under the metallographic microscope. The erystals of pyrite in the massive or softer ore are not so well cemented together as are the erystals in the harder type, but appear to be more dense and do not contain as much silica. The mineral has a very irregular pitted surface even after careful polishing, and the whole mass is made up of materials varying in density and hardness and also in the degree of cementation of their constituent parts; consequently no good pol- ished surfaces were obtained. Quite often the outlines of large cubes can be seen, but the pyrite constituting these is in very small erystals and may often be picked out with a needle point. Between these large cubical or irregular masses are distributed smaller patches of pyrite, which are generally hard and ean be polished. The remaining area is mostly occupied by very small erystals of pyrite mixed with dark silica. It is very probable that this portion of the ore is still in the making; that is, the pyrite has not replaced all of the rock and some of the more resistant materials are still present as a part of the ore. 18 Univ. Calif. Publ., Bull. Dept. Geol., vol. 3, no. 7, 1903. 1917] Clark: Geology and Ore Deposits of the Leona Rhyolite 375 A second generation of pyrite occurs in a very fine, dense deposit in fracture zones in the first generation. With this later pyrite small stringers of chalcopyrite and sphalerite have been deposited contem- poraneously. The second type of pyrite is much harder in character than the type just described, for it contains a considerable amount of silica between the partially developed erystals and between the irregular masses of the ore. Where the crystals are not in contact they are very securely cemented together by a siliceous matrix. Chaleopyrite of two generations appears in this pyrite; some was deposited with the pyrite and some has since been deposited along cracks, partially replacing the pyrite. Sphalerite and bornite are associated with the second generation of chaleopyrite and were probably deposited at the same time. One or two small stringers of chaleocite were observed along very small fractures in the chalcopyrite. The highly silicified country rock, containing a large number of irregular masses of pyrite of varying size, seems to represent the first stages of metasomatic replacement in the formation of the ore body. Genesis of the Ore-——Two general hypotheses may be advanced to account for the origin of the pyrite at Leona Heights: (1) It was deposited as a metasomatic replacement in the rhyolite by magmatic waters along a fracture zone. (2) It was formed as a metasomatic replacement in the rhyolite by cold descending solutions carrying iron sulphates derived from the oxidation of the disseminated pyrite. The first of these processes does not seem to have had any part in the production of the ore body, for if the sulphides were deposited by magmatic waters there would be evidence in the mine of hydro- thermal alteration, together with minerals that are thought to be the products of ascending thermal solutions; but nowhere in the mine has such alteration been observed or such minerals found. The second hypothesis appears to account for the ore at Leona Heights. Small deposits of pyrite formed by meteoric waters at ordinary temperature have been reported from numerous localities, the iron in many eases being supposed to have been derived from the ferromagnesian minerals, and the deposition of the pyrite in the present instance has been probably brought about by similar processes. It is thought that the ore at Leona Heights was formed in a manner analogous to that known as the process of secondary sulphide enrich- ment. The disseminated pyrite when oxidized at the surface formed 376 University of California Publications in Geology [Vou. 10 iron sulphate and sulphuric acid. These products having been carried down by descending meteoric waters to the ground water-level, or the zone of reduction, lost the free acid and the salt was reduced to pyrite. According to Emmons,'* pyrite oxidizes as follows: FeS, + 70 + H,O = FeSO, + H.SO, 6 FeSO, + 30 + 3 H,O=2 Fe,(S0,), + 2 Fe(OH), Ferrie sulphate then breaks down, forming ferric hydroxide and sulphuric acid. However, this last step is not always completed in the zone of oxidation, for the analysis of mine waters commonly reveals the presence of ferric and ferrous sulphates below the zone of oxidation. It seems probable that most of the iron sulphate is reduced to sulphide before the ferric hydroxide stage is reached in the process of oxidation, or else limonite would be produced, as pointed out by Emmons.'® He gives the following equations for this last process : Fe.(SO,); + 6 H,O=2 Fe(OH), + 3 H.S0, 4 Fe(OH), = 2 Fe.0, + 6 H,O=2 Fe,0;.3 H.O + 3 H.O It seems, then, that whatever the stage in the process of oxidation sulphurie acid is produeed. According to the experiments of Allen, Crenshaw, Johnson, and Larsen,** pyrite will not form in the presence of a strong acid solution, but weak acid or neutral solutions are necessary for the formation of pyrite at ordinary temperatures. They also conelude from their experiments that neutral solutions and high temperatures favor the formation of pyrite, while acid solutions and low temperatures favor the formation of mareasite. In the light of these facts it seems necessary to explain a method of neutralization of the acid formed in the oxidation of the pyrite near the surface. When the rhyolite alters it forms kaolin and silica. Both of these minerals are very abundant in the altered rock. The experiments of Whitman’ suggest the explanation of at least part of the neutralization of the free acid in the sulphate solution. They show that basic aluminum sulphate is formed and that pyrite is pre- cipitated as a result of the reducing qualities of kaolin. It is a well 14 Emmons, W. H., The Enrichment of Sulphide Ores, U. 8S. Geol. Surv., Bull. no. 529, p. 48, 1913. 15 Op. cit. 16 Am. Jour. Sci., ser. 4, vol. 33, p. 169, 1912. 17 Whitman, A. R., Vadose synthesis of pyrite, Econ. Geol., vol. 8, p. 455, 1913. 1917] Clark: Geology and Ore Deposits of the Leona Rhyolite 377 known fact that crystals of pyrite, according to Ransome,'® are found in and associated with kaolin, for kaolin is very abundant in the oxidized zone at Goldfield, and is also found in the sulphide zone, associated with quartz, alunite, and crystals of pyrite. He also states’? that pyrite forms a considerable part of the altered rocks, particu- larly the dacites and latites that have been altered to alunite and kaolin rock. In the Butte district Weed”? reports pyrite, sericite, and quartz as the chief minerals in the altered zones. Mr. Lindgren*? gives pyrite as a mineral formed in the zone of secondary sulphide enrichment by meteoric waters. The Relation of Fracturing to the Ore Deposit—The rhyolite in the vicinity of the ore deposit is intensely fractured, as shown in the mine workings. Along most of the fracture planes the fact of move- ment is shown by slickensides or gouge. The intensity of the move- ment along fractures has been doubtless due to the larger faults that traverse this region. The major fault traverses the valley to the west, while a minor fault, as shown on the geologic map, extends through the hill near the pyrite deposit. The development of this complex fracture zone has facilitated the passage of the meteoric waters through the acid porphyry in such a way as to cause the localization of the ore at this point. It is also possible that the two types of pyrite are the products of a continuous period of mineralization interrupted by faulting movement. The Reducing Effect of the Rhyolite-—The oxygenated meteoric waters descending through the intensely fractured acid porphyry would react on the feldspars in the wall rock, producing sulphates, kaolin, and silica, and it seems probable that by the time these de- scending solutions had traveled vertically and probably for some dis- tance horizontally through the rhyolite, which was then much thicker and wider than at present, they would have become neutral, or even slightly alkaline. According to Emmons,” acid solutions may become neutral, and even alkaline, in a relatively short distance from the surface. He says: ‘‘There is considerable evidence that acidity de- creases below the water-level. Analysis of two samples of water taken from a column of water in the Callaway shaft, Duektown, Tennessee, indicate a decrease in acidity of more than 50 per cent within a ver- 18 Prof. Paper, U. S. Geol. Surv., no. 66, p. 127, 1909. 19 [bid., p. 113. 20 Prof. Paper, U. S. Geol. Surv., no. 74, p. 90, 1912. 21 Heonomic Geology, vol. 2, p. 105, 1907. 22 Op. cit., p. 89, 1913. 378 University of California Publications in Geology [Vou. 10 tical distance downward of 37 feet. Some of the analyses from the Capote mine, Cananea, Mexico, show also a neutralization of acid at comparatively shallow depth. The geologic data are comparatively in harmony with this conclusion, for there is abundant evidence that descending acid waters attack alkaline or alkaline-earth silicates and alkaline-earth carbonates ; acid reacting with feldspars or sericite forms kaolin, and these reactions are attended by the solution of alkalies or alkaline-earths as sulphates.’’ It is probable that the sulphate solutions upon reaching the ground water-level, or the reducing zone, lost free acid and became neutral. The sulphate was then reduced to the sulphide and the pyrite-ore body formed as a metasomatie replacement in the rhyolite. From the character and disposition of the ore deposits at Leona Heights it seems probable that the rhyolite at this place is underlain by the Knoxville shale; indeed, from the exposures of this shale near by, as shown by the geologic map, it may be safely inferred that the shale lies at a comparatively short distance below the present workings in the ore body. The ore body described by Mace** rests on a carbo- naceous shale, and he coneludes that organic matter from the shale was taken into the underground circulation and produced a local reducing water table. The ore, as far as has been exploited, appears to have a downward trend or pitch towards the northeast, so that it may extend to the shale. The shale may have suppled reducing agents in the form of carbonaceous matter and H.S to the ground water. The downward percolating water contained in solution the metallic salts. The surface of the underground water was probably near the top of the shale formation and the water was suppled with carbonaceous matter and H,S derived from the shale. When the two waters met at the water table the ferrous sulphate was completely reduced to pyrite. If this be so, the influence of the shale on the chemical con- dition of the ground water may have been a potent factor in the local- ization of the pyrite deposit. Much light will be thrown on this point when the lower limit of the ore is determined, and the probability of shale lying not far below the present mine workings should be consid- ered in plans for exploitation at lower levels. 23 Op. cit., p. 1320. 1917] Clark: Geology and Ore Deposits of the Leona Rhyolite 379 SUMMARY The Leona Rhyolite occupies a narrow belt along the front of the Berkeley Hills from Hamilton Gulch at Berkeley to a point about five miles southeast of Haywards. It comprises a lava flow that probably followed an erosional valley along the contact of the Knoxville shale and the Franciscan. The rock is very much fractured and has undergone alteration by surface agencies. The rhyolite contains pyrite as an original mineral, the oxidation of which has colored the surface reddish brown. The rhyolite is probably Pliocene or older, and has been quite extensively faulted in post-Pliocene time, some of the movements occurring in very recent time. The petrographical study of the rhyolite shows that it may be divided into four distinct facies, based principally on texture. It shows a gradual gradation from glassy and spherulitiec through por- phyritie to felsitie facies. This supports the field evidence that the rock probably came from a common source and represents a single flow. The chemical analyses show that the rock is a soda rhyolite. East of Oakland, near Leona Heights, there are considerable masses of potato-shaped bodies of pyrite in the rhyolite. The metallographic microscope shows that there are two types of pyrite: one soft and massive, and another highly silicified and very hard. The ore contains chalcopyrite in very small quantities, which was mostly deposited contemporaneously with the pyrite. Traces of secondary chalcocite have also been detected. The ore deposit was formed as a metasomatie replacement in the rhyolite by descending meteoric waters. The ore body is in a frac- tured zone determined by a fault in the rhyolite which allowed free passage of meteoric water. The reducing condition of the ground water may have been induced in part by carbonaceous matter from the Knoxville shale that probably underlies the ore body at Leona Heights. EXPLANATION OF PLATE 25 Fig. A. Showing the ideal type of spherulite. The number of plates of feldspar that make up the spherulites are so small and are in such large numbers that the outline of each individual plate is not visible. X 230. Fig. B. Showing the spherulites in the ground-mass and in the altered rem- nants of phenocrysts. The prismoid crystals that make up the spherulite are microscopic in size and do not give a black cross under crossed nicols. X 60. [380] UNIV CARE. (PUBIE BULEY DEPT: GEOL: [CLARK] VOL. 10, PL. Zo EXPLANATION OF PLATE 26 Fig. A. A characteristic section of gouge surrounding the soft type of pyrite. It generally contains much pyrite and always shows evidence of movement in the breccia fragments included in it. Natural size. Fig. B. Showing the metasomatic process at work in the formation of the hard type of pyrite. (&) Silicified rhyolite. (S) Sulphides. Natural size. [382] ey AAS) 10, [CLARK] VOL. DERimGEOIE GAEIE, PUBIED IBUIEL, UNIV, [CLARK] VOL. 10, PL. 27 ANS NS (mais), faistg RiP ANN a e C LZzZ » 2 ae + : i ao e ro. * FIC iS RYe, BAG)». «Eargasm hur " . soutTHERN : e Pleistocene Recent PO rece rN _ SanAntonio Temescal Formation Formation With Chert-Gravel member Qsac MATIONS Geology by C. W. Clark Surveyed in 1916 {CLARK] VOL. |0, PL. 27 UNIV. CALIF, PUBL. BULL. DEPT, GEOL. pricirerar aire Ss GE eS ey, pl ee 2 Sal SCD ~~ eon) in Z ES %, &, fi SS =: or ye a Nii = 0 fas = y 5 =: Sowa at = = Sf o i ? ET K pA Th 2) uM SSR ERE: Vv, ? = = 5 S = | BI oy a0" PLL T = Bu i if Baer Sal if G A S resis: . iD The re ; Opes Pe . tL AAY + nA by 1 Osa} | i} 1 A = NGM ji 2 a << Berkeley E 5 , Waa | ear | Se ENGY, > + WESTER! = ) mi yd He 7 BoB! ant + \Q:, Elmhurst - G vv s0uTHERN,.* Ie lel inn ear tl) tee 2 . Gat oo Z JURASSIC Lower Cretaceous Upper Cretaceous Pliocene (?) Pleistocene (a > fs c a) ‘ Te s SN | FA dsa at Kk Ko Tir! TH ; < | oie Cc é S\N 3 rol : 5 Franciscan Group Knoxville Shale Oakland Conglomerate Chico Formation Leona Rhyolite San Antonio renee Formation Sy Marae le X Stone Quarry A Dip and Strike Formation ® Pyrite Mine ——— Fa With Chert-Gravel member Qsac GEOLOGIC MAP OF LEONA RHYOLITE AND ADJACENT FORMATIONS Tir KK Ko Ke ° 1 2Miles Stslet Cae Contour Interval 100 ft. Scale of Sections i : mae Topography Adapted from U. S. Geology by C. W. Clark Geological Survey Sheets Surveyed In 1916 November 27, 1917 2 | FORMATION IN THE VICINITY fae COLFAX, CALIFORNIA BY CLARENCE L. MOODY | | RA spa UNIVERSITY OF CALIFORNIA PRESS BERKELEY : eg UNIVERSITY OF CALIFORNIA PUBLICATION 6 Norge.—The University of California Publications are offered in exe: te foe Toe eations of learned societies and institutions, universities and libraries. Coniplete i all the publications of the University will be sent upon request. For le «co pice publications and other information, address the Manager of the Unive . Press. © California, U. S. A. Ali matter sent in exchange should be address: 15 The © Department, University Library, Berkeley, California, U. S. A itty Orro HARRASSOWITZ R. FRIEDLAENDER & SOHN LEIPzI@ BERLIN Agent for the series in American Arch- Agent-for the series in American aeology and Ethnology, Classical Philology, » aeology and Ethnology, Agricultural Sciences Economics, Education, History, Modern Botany, Geology, Mathematies, Pathol Philology, Philosophy, Psychology. Physiology, Zoology, and Memoirs. ~ , Geology.—ANDREW C., LAWSON and JoHN C. MERRIAM, Editors. Price, volumes 1-1, $3.5 volumes 8 and following, $5.00. i : Cited as Univ. Calif. Publ. Bull. Dept. Geol. Volume 1, 1893-1896, 435 pp., with 18 plates, Price ...s..cssssssssssczssessssnsesessssnseeesesteeaeebBs Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price ........-----.-. Volume 3, 1902-1904, 482 pp., with 51 plates, price -.....-..-.--.s:cesccessceseesce-e s Volume 4, 1905-1906, 478 pp., with 52 plates »price! 2.200222 eee ‘ Volume 5, 1906-1910, 458 pp., with 42 plates, price -....-...2.-c------ccese-ceecenseneeereceneceensred A list of titles in volumes 1 to 5 will be sent upon request. VOLUME 6. . The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller... Sa . Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern ~ Nevada, by John.C. Merriam. Part I.—Geologie History......:..22..2 Rises: scenes The Geology of the Sargent Oil Field, by William FP, Jones .... ih eceeeeeeenaee : Additions to the Avifauna of the Pleistocene Deposits at Fossil Lake, Oregon, by Loye Holmes Miller. op: .0....20 2c. scncitynccesceesnpeeabesteee esto nseenzsel ent can 5. The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Reid 6. Note on a Gigantic Bear from the Pleistocene of Rancho La Brea, by John C. Merriam. 7. A Collection of Mammalian Remains from Tertiary Beds on the Mohave Desert, by John C. Merriam. Pe poe Nos. 6 and 7 it One, COVEN» ...-2i-.:..:ceqeonesotveceesee sesaceecnenedecneencesate de seh ’ 8. The Stratigraphic and Faunal Relations of the Martinez Formation to the Chieo aud Tejon North of Mount Diablo, by Roy HE. Dickerson ~.....2222-ie-cessctenceetemeeeee 9. Neocolemanite, a Variety of Colemanite, and Howlite from Lang, Los Pees aK County, California, by Arthur 8. Bakles we ; 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. Taylor... ot a 11. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern * Nevada, by John C. Merriam. Part Il.—Vertebrate Faunas -....2.2.----ceceessee-e 12. A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, by Loye Holmes Maier... neneee tion soaeee Ree aS ee Haven ood Sete ae As, aU eee er 13. Notes on the Relationships of the Marine Saurian Fauna Described from ‘the Triassic — of Spitzbergen by Wiman, by John C. Merriam. 14, Notes on the Dentition of Omphalosaurus, by John C. Merriam ard Harold C. Bryant. Nos, 13 and 14 in one cover. 2. :21:) 520-2 eotegth Eee ee ; 15. Notes on the Later Cenozoic History of the Mohave Desert Region in Southeastern California, by Charles Laurence Bakker ..<..22:..c2-c2icfescey--necenoeversees™a raped eee ee 16. Avifauna of the Pleistocene Cave Deposits of California, by Loye Holmes Miller . 17. A Fossil Beaver from the Kettleman Hills, California, by Louise Kellogg ...... 18. Notes on the Genus Desmostylus of Marsh, by John C. Merriam ............0......-- BS 19. The Elastie-Rebound Theory of Earthquakes, by Harry Fielding Reid .................... VOLUME 7. 5 1. The Minerals of Tonopah, Nevada, by Arthur S. Halle... 03.3 ee 2. Pseudostratification in Santa Barbara County, California, by George Davis Louder- Dale > a. ran. So denn te nascar noch bicep et cosets suawoplemt anand teas a pee ene ee ar 3. Recent Discoveries.of Carnivora in the Pleistocene of Rancho La Brea, by John C. Merriam: ig) o. 2. . oh sceecenensnttssculecggpconetasecueassansneteas anaes sapiens ene Saas i a aia es ae ee = aa 4. The Neocene Section at Kirker Pass on the North Side of Mount Diablo, by Bruce Tn, Clark), sc2cnccee eke a ae ee | 5. Contributions to Avian Palaeontology from the Pacifie Coast of North America ue Loye Holmes Miller dettestSbase venenccbpenaesoni ge sendecrare ov stenaoe dpsed sees=es ese oases ae aceon eae eS UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 21, pp. 383-420, 4 text-figs., pls. 28-33 November 27, 1917 THE BRECCIAS OF THE MARIPOSA FORMATION IN THE VICINITY OF COLFAX, CALIFORNIA BY CLARENCE L. MOODY CONTENTS PAGE OVER YGHBUCH KON eet ee ace Nef ea gee Pe 383 MO CatTommMam dnyt OO Sma ys ss etek Ms eon en eae ese asc cet baays dans bos cp lees ececsatessseeedeteeeest 384 Gere nA COO Gay gree te atte PE R LE oo i ce ods cacece sects deecedcecccteecesens ssbeccecseteseseadeebese 386 Stratigraphy of the Mariposa formation -........2..2.22..2..202-.22-c2220cete 0 eee eeceeeeee eects 388 (Cremfenallest ave Tle ibaa teers ote Serra ee ee as ees eats ee oe 388 PSTN GS acest act a eo eee 389 PSEA TIGTSA ACLS) ace ca i PE PERN nee ae 1°) () TBR RO COGN > sore rate a ep 391 OccumrenCemeentetreta ete eE 391 Megascopic features ............ Beh ener lean Pees eh ce Sere ee Be DO Microscopie feat UTES: 12.2222. -..c.cecce tl coc ee cece teceneeteeenneeencen sens Ua Sia) hs ee 397 Breccias in other areas of the Mariposa —__.......---2-2---c:c-ce-ceeeceeeeeeeeeeeeeteeeeeeeeeeeeeeees BOT ANAC ONIGOLO BIC CVAC ENCE ine. cee iene csesa ct etsncscecedenccsacedcccnsteceeser-ctenceseecesdsceiseceeesscsescones B98 Classification of related conglomerates _..........2.---2-.220c2ece-cceceecceceecceceeceeeeeeseteneeeeeeee 399 (GermenamStarbeme mis m-smeercecet cscs cee ssc. as e8e 28sec slot ce sate Coscccceueccacseecedecaotsuatécieteselsetee 399 BIW Ireasngi 0a © Win ees ees ate Wee ee Nee oe A oc e coe ee ee fe Foes set cgav seeder atl: wedshthan Secste 400 TEP ea Uh a ek oo a 401 (GST OTE eee ka re 9 a 402 HEUTE TN CTA CS ape re Noe ce ales Mec ee Sa sees ee rae eS oe gta ed Sen ea ee 405 Erobableomigin of the Breccia .2...2.-.---.-----ctec-cc-tecccececececeeceecdecceceeesecaeceseecsaeceiecsenaterss 406 SI BIPUEQIEL TS) cs ay ere AP a 410 Memeousmocks) in) whe: Miarip OSes 2e..cc.cee-c2:eectceccteceseccseecectececectecee-cectsvecteeceeans-eseeceeeeree 413 I RSIEUW INS) i ep aS OR et aOR onc a ees 413 INTRODUCTION The Mariposa formation, which has long interested students of the Sierra Nevada, is exceptionally well exposed in the vicinity of Colfax; it is believed that a more favorable locality for the study of its stratigraphy will not be found. 384 University of Califorma Publications in Geology [ Von. 10 The present investigation was undertaken in the hope of securing definite evidence concerning the origin of the uncommon breccia beds which comprise about one-fifth of the formation in this vicinity. The main purpose of this paper, however, will have been accomplished if the attention of geologists is sufficiently called to the peculiarities of these beds to inspire a further investigation as to their origin. The chief stimulus that has lent zest to the investigation has been the sug- gestion by Professor A. C. Lawson that the breccia may be a Jurassic tilite. While the results obtained only partially support this view, its value as a working hypothesis is acknowledged with pleasure. Free use of the folio of the United States Geological Survey cover- ing this region has been made during the prosecution of the work. LOCATION AND TOPOGRAPHY The region studied hes in the southwest quarter of the Colfax quadrangle, California; it embraces an area of 60.5 square miles, with a length of 11 miles and a width of 5.5 miles. The accompanying map (pl. 28) shows the general features of the geography. Colfax, the only town of importance in the vicinity, is about sixty miles northeast of Sacramento. The small area shown on the map is part of the foothill belt of the Sierra Nevada. The relief is pronounced and rapidly increases in ruggedness to the north and east, attaining a maximum at the crest of the range, about thirty miles northeast of Colfax. The highest eminence in the region under consideration is on Cape Horn Ridge northeast of Colfax; its elevation is 3100 feet. The lowest point is at the bottom of the canon of the North Fork of the American River ; the 900-foot contour erosses the stream just south of Owl Creek. The maximum relief is thus 2200 feet. The dominant features of the topography are the canons of the Bear River and of the North Fork of the American River. The Bear River takes its course diagonally across the northwestern corner of the area mapped. It occupies a large rugged canon, with precipitous walls where the stream cuts through the plutonic mass northwest of Colfax, but with more gentle approaches in other tracts. Its chief tributary is the Greenhorn River with a small catchment basin west of Dutch Flat. The average grade of the Bear River within the limits of the map is 71 feet to the mile. The North Fork of the American River occupies a deeply incised trench with an average slope of the ley As 10, [MOODY] VOL. UNIV, CAMIE, PUBL BUEE. DEPT: GEOL. — Se / ae | —— Vv 4 i Fk Vv XxX Diabase — ~ Calaveras Mariposa Superjacent Series Amphib- olite Serpentine Gabbro gion ax Re eologic map of the Colf G Seale: 1 mile 1917 | Moody: Breccias of the Mariposa Formation 385 walls of forty degrees. Little difference is to be found in the rate of erosion, measured in terms of steepness of slope, in the canon; amphibolite seems no more resistant than the slates of the Mariposa. A great number of youthful, tumultuous streams are tributary to the North Fork. Robbers Ravine and the nameless gorge just east of Colfax drain the rugged region around Cape Horn. South of Colfax the drainage is chiefly into Bunch Canon. Live Oak Creek, a tributary of Bunch Creek, and Bushy Creek, which flows directly into the North Fork, drains the high region around New England Mills. The eastern tributaries are Indian Creek, Bushy Creek and Owl Creek, all drain- ing the Forest Hill divide just beyond the limits of the map. The average grade of the North Fork of the American River is 58 feet to the mile. The disparity in grade between the Bear and the American rivers has been shown by Lindgren to be due to the weakening of the activity of the former caused by the capture of its headwaters by the South Fork of the Yuba River in the vicinity of Emigrant Gap. At least two cycles of erosion, separated by a period of extensive deposition are represented in the region, and each controls in a greater or less degree the development of present physiographic features. The first eyele appears in the old surface upon which the superjacent series was laid down. This surface has been extensively exhumed by the stripping away of the gravels and voleanic rocks which have accumu- lated since Cretaceous time. The surface is one of subdued relief carved in the massive, schistose and slaty rocks of the basement com- plex. The remnants of the superjacent series which are found on some of the hills determine a second surface of low relief, but of a totally different character; it is a graded, depositional surface. The present topography was evolved by the dissection of this graded sur- face by streams consequent upon a late uplift of the Sierra Nevada block. The present elevation of the range may have been attained in a double uplift, the first stage of which caused the removal of most of the superjacent series, and the second instituted the vigorous erosion that is still continuing in the carving out of the narrow, groove-like cafons in the basement rocks. The present streams flow in V-shaped trenches with abrupt approaches; lateral or tributary drainage has not been sufficiently advanced as yet to remove all of the once extensive superjacent series; outliers such as Howell Hill and Colfax Hill are abundant and characteristic of this, as of other parts of the foothill belt of the Sierra Nevada. In a word the present geomorphic cyele is still in a stage of early youth. 386 University of California Publications in Geology [ Vou. 10 GENERAL GEOLOGY The geology of this small region is typical of the foothill belt of the entire Sierra Nevada; all the rocks, except granite, commonly found on the lower slopes of the range, occur within its limits. The oldest rocks shown on the map belong to the Calaveras forma- tion. In the foho of the United States Geological Survey covering this region five divisions of the Calaveras have been recognized, but for the purposes of this paper the general term Calaveras suffices. Four separate areas appear on the map. The formation west of New England Mills consists of a highly compressed series of black, clay slates and dark, argillaceous sandstones with several lenses and beds of limestone and bluish or grayish chert. The smaller area northwest of the Bear River is lithologically similar. Intermediate between these two localities on the east bank of the Bear River, directly west of Colfax, is a small outcrop of slate and shghtly altered sandstone over- lain by a thick mass of gray limestone which bears several species of lower Carboniferous fossils (see section EF, pl. 28). Forms referable to the anthozoan genera, Clisiophyllum and Lithostrotion, together with round erinoid stems were collected, while two species of Plewro- tomaria, and one or two spirifiroid brachiopods were observed. In the northeastern part of the area the Calaveras rocks are fissile clay slates of a brownish to black color with a phyllitic development of mica, which gives them a lustrous, silvery aspect when weathered. The Mariposa formation of Upper Jurassic age succeeds the Calaveras. It is generally regarded as the latest sedimentary forma- tion of the Bedrock series. The area shown on the map represents the northern limit of a long belt of the formation traceable from Mariposa County. In this vicinity it consists of black slates alternating with dark gray sandstones and a great number of breccia beds. Its strati- graphy will be considered more at length later. Teneous rocks are abundant in the area. The amphibolite belt which the American River canon follows closely for some distance may represent flows contemporaneous with the deposition of the Mariposa sediments; long, narrow lenses of black slate included within the amphibolhte, near the toll-house on the Forest Hill road, suggest this contemporaneity. Southward, however, and just east of the limit of the map, dikes of a material in every way similar to the amphibolite of the main belt clearly cut the Mariposa slate. The diabase west of Bear River is regarded by Lindgren as repre- senting lava flows possibly antedating the Mariposa depositional epoch. 1917 | Moody: Breccias of the Mariposa Formation 387 Part of the diabase is certainly irruptive, however; dikes of a por- phyritie facies clearly intrude the Calaveras limestone shown in sec- tion EF, and other dikes may be seen crossing the Mariposa contact where exposed by the excavations for the Bear River canal. Numerous diabase dikes are included wholly within the Mariposa formation. Serpentine, in dikes and masses, cuts the Mariposa and older formations. Its occurrence in dikes along contacts of both igneous and sedimentary rocks suggests that it represents a late phase of intrusion. The planes of schistosity of the Calaveras were, however, seen to pass obliquely across a serpentine dike near the Bear River, Soil and Alluvium Superiacent Series (Tertiary ) DB Mariposa (Jurassic ) DB SP GB Calaveras (Carboniferous ) AM, Amphibolite; DB, Diabase; SP, Serpentine; GB, Gabbro. Fig. 1. Generalized columnar section though other areas are wholly unsheared; the possibility of two periods of serpentine intrusion is thus indicated. The elliptical area of gabbro, northwest of Colfax, is a coarse granitic rock of basic aspect, which has invaded the Mariposa, the older diabase and the Calaveras. The mapping suggests that this gabbro was brought into its present position by anticlinal folding, but its irruptive nature is indicated by chilled margins and discordance with the strike of the sedimentary beds. The only other rocks in the vicinity of Colfax are the voleanie tuffs and river gravels of the superjacent series, which appear as outliers on the higher eminences of the region. 388 University of California Publications in Geology [ Von. 10 STRATIGRAPHY OF THE MARIPOSA FORMATION GENERAL STATEMENT The Mariposa formation is familiarly referred to as the ‘‘ Mariposa ’ and this term is justified when the two long belts of dark sediments, stretching from Mariposa County to well north of the Mother Lode are considered. In many localities, however, coarser sedi- ments are interbedded with the slates; thus in the Colfax region not over half the rocks of the formation are slate. Sandstones and grits are here well differentiated from the typical black, slaty argillites. Both within the slate and within the sandstone occur numerous beds slates,’ of angular breccia and subordinate conglomerate lenses which persist on the strike and form bold ridges in the differential weathering of the series. It is estimated that one-fifth the volume of the Mariposa beds shown on the map is made up of this coarse material. That the Mariposa formation as mapped is a stratigraphic unit cannot be denied. The relation of the breccia to the slate in the immediate vicinity of Colfax is somewhat obscured by the regolith as well as by minor faulting; but the sections exposed in Live Oak Ravine, in the American River canon and on the Forest Hill road in Bunch Canon, clearly show a conformable series of slates, sandstones and breeecias interbedded and in places grading one into the other. Columnar sections were made in the field showing the sequence of beds in Bunch Canon and in Live Oak Ravine. gives a good description of the rock. It consists of a great variety of types and sizes of boulders with very little sorting in evidence. Large, isolated boulders sometimes occur in clay slates; the larger masses are usually rounded or subangular, some are markedly angular. The matrix is ordinarily graywacke with an occasional slate pocket; numerous particles of quartz, feldspar, chert and felsite are to be seen under the microscope. Some fine-grained turbid matter in the matrix contains chlorite, thus differing from the Dwyka. Within the deposit, sudden lateral and vertical changes often occur; shales are frequently interbedded with coarse material; quartz- ites, rapidly grading into akrose, interdigitate with the coarser facies. Coleman*® describes and figures well-preserved striations on some of the boulders; they show best on felsites and fine-grained greenstones ; many of the surfaces are well polished. In the Cobalt tillite it has been possible to differentiate various types of glacial debris; thus widely separated fragments in a medium-grained matrix indicate ground moraine; wholly coarse material is considered as representing the terminal moraine, while various aggregates of rudely sorted, rounded pebbles mark the sites of ancient kames. In arriving at a conclusion as to the origin of the Cobalt conglomerate, Coleman con- sidered and rejected hypotheses involving crushing, faulting, talus formation, and exceptionally heavy-river currents. The tillite is inter- bedded with slate layers up to five hundred feet in thickness, which are considered to represent deposition during interglacial periods. The formation stretches over thousands of square miles and thus probably indicates the extension of a great ice-sheet over the continent in that remote time. Other ancient tillites in America have been found by Sayles?’ in 24 Coleman, A. P., Jour. Geol., vol. 16, pp. 149-158, 1908. 25 Hore, R. E., Jour. Geol., vol. 18, no. 5, pp. 459-67, 1910. 26 Loc. cit. 27 Sayles, R. W., Harv. Mus. Comp. Zool., vol. 56, no. 2, 1914. 1917] Moody: Breccias of the Mariposa Formation 405 the Boston Basin, and by Atwood?’ in the Eocene of southwestern Colorado. The probability of a glacial origin for the Mariposa breccia will be considered later. FANGLOMERATES This term was proposed by Professor Lawson?® as a petrographic designation for the coarser portions of alluvial fan formations. Aridity and high relief are postulated in ascribing a fan origin to a deposit. The constituents of a fanglomerate range from the coarsest material down to fine sand. Blocks of extraordinary size are apt to appear at the apex of a fan, and occasional ones, a foot or more in diameter, are found far down the slope where the average size of the material is less than one inch in maximum dimension. he UNIVERSITY OF CALIFORNIA PUBLICATIONS Nore.—The University of California Publications are offered in exchange ‘for eations of learned societies and institutions, universities and libraries. Complete all the publications of the University will be sent upon request. For sample copies, publications and other information, address the Manager of the University Press, Ber California, U. S. A. All matter sent in exchange should be addressed to The Exe Department, University Library, Berkeley, California, U. S. A, Ke Orro HARRASSOWITZ R. FRIEDLAENDER & SOHN LEIPZIG . BERLIN. - Agent for the series in American Arch- Agent for the series in American Ar aeology and Ethnology, Classical Philology, aeology and Ethnology, Agricultural Sciex Economics, Hducation, History, Modern Botany, Geology, Mathematics, Pathol Philology, Philosophy, Psychology. Physiology, Zoology, and Memoirs. Geology.—ANpDREW C. LAWSON and JOHN C. Merrgiam, Editors. Price, volumes 1-7, $3.5) volumes 8 and following, $5.00. : Cited as Univ. Calif. Publ. Bull. Dept. Geol. Volume 1, 1893-1896, 435 pp., with 18 plates, price .....-2....s:cce-cenecescsecesenseneeeeeeoeeee - Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price ...-....1.--c-e-cc-ceececsee-oreee Volume 3, 1902-1904, 482 pp., with 51 plates, price ........ ieee ttcselee scheme thet ee Volume 4, 1905-1906, 478 pp., with 51 plates, price .........-ccscccczscseneccncnsneearenenseecseceneens Volume 5, 1906-1910, 458 pp., with 42 plates, price -.......2.-2.--------ceec-cecceenccenenesseusenseered A list of titles in volumes 1 to 5 will be sent upon request. VOLUME 6. . The Condor-like Vultures of Rancho La Brea, by Loye Holmes Miller...................-... ‘1 . Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern Nevada, by John C. Merriam. Part I.—Geologie History...........22-..-----.c-sceceececseceeeeee The Geology of the Sargent Oil Field, by William F. Jones .....2...2...2-2c..e--sceeceseescoceee Additions to the AVifauna of the Pleistocene Deposits at Fossil Lake, Oregon, by Toye “Holmes. Miller »._..-2. c._--2s--.:sceze-nctece oni nennrocenecbatenesaguats ecehae = epee . The Geomorphogeny of the Sierra Nevada Northeast of Lake Tahoe, by John A. Reid, . Note on a Gigantie Bear from the Pleistocene of Rancho La Brea, by John C. Merriam. . A Collection of Mammalian Remains from Tertiary Beds on the Mohave Desert, by John OC. Merriam. ; os. 6, and 7 iM One: COVER? 22.2 -2.2..-csncstensconteatens=ecoeeontncepstasnecpun sete aee anes teeeeeeeeae aaa 8. The Stratigraphic and Faunal Relations of the Martinez Formation to the Chieo and Tejon North of Mount Diablo, by Roy E. Dickerson .......0...0.2-1-1c2-2steeeeeeeeene 9. Neocolemanite, a Variety of Colemanite, and Howlite from Lang, Los Angeles County, California, by Arthur S. Hakle 2.-2.203.2 05-2 cecc-ptetecocen ence ee 10. A New Antelope from the Pleistocene of Rancho La Brea, by Walter P. Taylor... 11. Tertiary Mammal Beds of Virgin Valley and Thousand Creek in Northwestern Nevada, by John C. Merriam. Part II.—Vertebrate Faunas ..............---.:s00ce-ceseccees 12. A Series of Eagle Tarsi from the Pleistocene of Rancho La Brea, by Loye Holmes IMAM eb s2sct Se Seen BS olo an cn econ cnet ndens ost tncwatetiesneentosstewlet otters sen te ae See 13. Notes on the Relationships of the Marine Saurian Fauna Described from the Triassic — of Spitzbergen by Wiman, by John C. Merriam. 14, Notes on the Dentition of Omphalosaurus, by John C. Merriam and Harold C. Bryant. | Nos. 13 and 14 in one- cover, :....2-s:--.1.2225 ee ee 15. Notes on the Later Cenozoic History of the Mohave Desert Region in Southeastern California, by Charles Laurence: Balcer, \i2.22. on. ac..ccssescn-oce see ectonneshone ses hes ae eee 16. Avifauna of the Pleistocene Cave Deposits of California, by Loye Holmes Miller... © 17. A Fossil Beaver from the Kettleman Hills, California, by Louise Kellogg ................ 18. Notes on the Genus Desmostylus of Marsh, by John C. Merriam ...............--sesceeeserecenone” 19. The Elastic-Rebound Theory of Earthquakes, by Harry Fielding Reid ..............-...... : VOLUME 7. 1. The Minerals of Tonopah, Nevada, by Arthur S. Hakle _.....-.n..--sscescseeesrns-csstenseereons 2. Pseudostratification in Santa Barbara County, California, by George Davis Louder- | Cy) Sa aa ee Rem SORT ore ML BNI DAE ye cen ee ( 3. Recent Discoveries of Carnivora in the Pleistocene of Rancho La Brea, by John C. Merriam”, 725, s-_s Ab Sie ne ee ee f 4. The Neocene Section at Kirker Pass on the North Side of Mount Diablo, by’ Bruce S Brags 6 Co) gma os an RO nr RMN ee He esc ney tt Ua 5. Contributions to Avian Palaeontology from the Pacific Coast of co Anciiea Loye.Holmes: Miller «2.02225 35.02 2 Soc. 8 cee UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 23, pp. 445-459, 1 text-figure, pls. 34-38 January 31,1918 ANTICLINES NEAR SUNSHINE, PARK COUNTY, WYOMING BY C. L. MOODY anv N. L. TALIAFERRO CONTENTS PAGE AIBC Aiba Mn aerate eens Snetee ere ce es Sec ced. Soe te fo en tabee a ope 8, Seas saseseccteed teas dueassadesesieci Sota 445 TESUGT SOREL ee ean ae a RS RS RT ener 446 Beats Vel OU SVU O My Kase ors eae aera ed eee RSs ee Lace solutes Lain ode scek sc duu a ceesdced nee seuedeevesneds 446 Hah SlOPmAp MyseaNG AATAIM Ae 12 28e o.oo c. Eee css See ceescsectaceg ss oxsectgeasvessencePecascuscunesnenss 447 FSRIB EW 1a) A er a a =e nS a) BREN tet @ CUUTGit) OTe reece teeny oy coven, wuweaue Sree, Meee eee ee oe esos agleses, oeevo sere area 449 (CCLACCOUSM SY SLOMMN tere crac atertet orcesael ooh cruesseetleg eves evseeciie sect. 2edesuse. Seeeeures Senbesditesads 450 @lowenlvatOrmia tomy kf eee ce ea cee ect Pao tec cece ese eve scateccgesatiecte 450 dhermopolisushalley ssa esse oe eee cat Pane oases coee cece ee eee eo ease dee ey 450 AViOsTayge Sn aill Ch aescess ste eseen cas cok ocd Se ccke sa cce Seedte secsceeeaccacececpsteraesurocoes eoterseuterucsen beseuece 451 LENORE ES OF OD aA OAR ee nen 453 (Gaye SN i ee a PB 454 VIC SA VET COR SONI Atl OMe. A scatetscee-cctcestc: iesatecese¥ccraae Sesezeseeoseeeeee he = cx Steet oe eaceseccls 454 Mena Sy SLOI esses emai Hee. ORE SO Ee a Bee 454 Wasatch formation. .... 454 GO traitenmanay Si SOM see cent seis ee Seteee test cpeec tte) secs Se eee ee ceceee esse ec 455 ANY SESTEEE (XE © TERT: SASS Ps SP PP Pr OP ee er 455 NUTT ya geet eae ee Oey er 455 SUC CUI CM se Senta fat coz ce acet secseceetveeca vst ens cuca rete ees Ses lenses les eas coheed oo be aasedeeanntipecceseeiee 456 ESRD EY SU Uta Sy, EE ae CU OCS ee a 456 Goosebetinga OTeeKsic NUICMN C822. fa. os eee ee ec A ec 457 CCOlO sien StO ty, ee smear nes tee teers tnat, oe bn- esctset a tescteeees fo suede: ese Sire. ee Meee 458 PROM AAV gO CTO C0 feece: s:cesYecncs ott ccateastscscnad caves aascacsceeentenscete-scesusi¢fcsteveel socteteute Menssceces 458 (COT epee 2 OX 0 eee 459 MSS ITTIATIN TV a eee cs eevee case, see Pabst a. Se esate eee led asec cgazene cectas defied dugecscecnccvsbieseset ve 459 LOCATION The area described in this report lies in Townships 46, 47, and 48 N, Range 101 W, along the western edge of the Bighorn Basin and in the southeastern part of Park County, Wyoming. All but that 446 University of California Publications in Geology [ Vou. 10 portion of the area south of Redtop Mountain is included in the south- western part of the Meeteetse quadrangle. The nearest railroad point is Cody, on a branch of the Chicago, Burlington and Quincey Railroad. Sunshine postoffice, fifty miles from Cody, may be reached by stage to Meeteetse, and thence by private conveyance (see fig. 1). M Ihe =p ee a 1 DAKOTA =e LARAMIE : NEBRASKA |SOUTH Fig. 1—Map of Wyoming, showing location of area described. FIELD WORK The field work on which this report is based was done in the early part of July, 1917. Tapir Remains from Late Cenozoie Beds of the Pacific Coast Region, by John ©. Mer rata. 25.2 a, senna getcne yp von snnnae Sete bance thats oe oR Se Soop ae The Monterey Series in California, by George Davis Louderback -:eccesceeccneseeeeeenente John C. Merriam . wecteewenceedetcdnoesen lea: Sieadscevtesstecs-s bagt =p Gen ee err A Peculiar Horn or Antler from the Mohave Miocene of California, by John Cc. 1 PUAN: *..cogcdenncednaatse Suede rasceekuze ST a se, MR eR Ne Chester Stock?” 2.22.05. esht it ove acca cee ac been came aie pease ©. Merriatn iis 26 ees ee Ss ae ae an of Rancho La Brea, by Reginald C. Stoner --..2...22.22 52-3 ee Merriam dal pdcnencedactedeoncdedpeecnacte ghle-opeee tooe ao een eee RS Desert; by John C. Merriam... 720 215 eee oes ee ‘Stee Ree Fi UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 24, pp. 461-515, 32 text-figures. Issued April 23, 1918 THE PLEISTOCENE FAUNA OF HAWVER CAVE BY CHESTER STOCK CONTENTS PAGE TE TaN SONORA ck ee eee 462 HGS HOM ygrO TNL CVIOUS #INVEStLO AULONS 3. oe cee cece cece c ares na caren cerer mentee sneneccnsnatveceec-reee 463 OC uIOMMO talela wivieTm CAV pte ate een eet nee ete Meee oe ost td sol s5s oueess cuerunseEaesecste 464 RelatLOTIMOtacayv.e sto: LOPOPTAphy, -.-ceiecee nn eee a ca cc edewsucenveceasences 464 iEmeseivattom vot. vertebrate LeMans 22-25. -- aos. 2 hens cance cee acct sawecea wes ceeecesnsseceeseeeenee eee 466 Oecummencee otwibiim anes Crain Gye eee ance ean a a ev cececen se baecencastseees 466 Jhitppraanras Uy EEE DEEN Sa ae ee eg Ee 467 Comparison of California, Cave tfaun as: .-2:..c-cceecs--ccscrsencceccnces ona cececazes cute svnsnessussaecsee 469 Comparison of the Hawver Cave fauna with the faunas from Port Kennedy Weposity and Conard Wissure i sli YN acai cecceensencceasetecattens 472 Comparison with Rancho Ia Brea, faunas”... ..--....-2.---22s--.se-cecece tee eeee tee tceeeeceenseenee 474 Companisonimwath Recents fauna 8 state Ee ok cadesacencadeadevedstanusenesouanses 475 IBICOLO CUCAIMCONSTOCEALIONS Hesse sce see ee tenes. can cee cet ts asan ss Jettuee sauscact oapite seca ce decndecleteeeeet 477 WES CTU TLO MMOL EMMA LENT Al sot nn fc. e oe ace as stat etans chee ceca ccuacteocehsodeatscocesuecdetsecsesdacanssensanteciecens 478 DETREI GAOT: eek ese al Oe Re ne 478 CSXHEY OETA NSE, J OTOYSISHT 0) 0 7 ef) Oo re i ae aE 478 (FED TETAITA YO 152 pests eee sae ees ee cn saeco a sp act ec acuet Saeacstedesshnanseceaceaseestosucseees 478 COPEITUA GLENS) aera ee ll a RE eee 478 Camisten Came Oi TiSa Wel Yees.ccre sete sveceas loses cel Sea cece sn cceee oa as cence eee aes 478 Warm SiaO Chic OPUS sISCHSCHOUGZ xecces cases sesenecoseces see teceeate neces edeceeeeceteccsecancee sueeeeeeeeaee 479 Mirate ale 50.0 OM: e Cmeseeeoee tae see rte te fee Oe Seer coe k coa5 cc ath ssc cb ese saetes eee oe 480 Sr OG OVA (G2) ios iS st eatece sooth cnc caceen aces csavscetocracgndtvacbagusieasea cuccceceaesteesuciasnoeoecnacncstaness 480 DEN SSSEN SG yer a 482 PL OVISMPN DWV CL Ieeetl ay SPs eset saa ctcace crea, Sen teeee een a sens hv. torso aosqcecesatet coe tencieee lee eteeeeteses 482 ISIS MLO Dalb liye nis [sj sereer teeter etn as SUE M2 ee Be 483 DROS ES SUIT Ae ee cea ER PC oe RPP EES aU 486 INCOR UES = EWES T Cao Nef gl St Uh ae ee 486 INSOLES SH a esa ge Sore Te 487 NE OPUS LOD AID liygeN pS P syaees tessa cacacebesdes secadsac0e_facecs sndee see Cuncsnceanns ence eectSeee eet 487 IB e rate maces seee. cea neon eekotss USN EL cies ee sae en es 488 Mayo donmphanlanigg@ wets se. 7 rte) ane ce Ree eee ea eee eerie ease cn 489 Mire prailonivx (Gish isp sgte titass ocr. treats ofeee ste ccat Nee acuetiuest ccs suteus esse ee AE 491 Nothrotherium shastense hawveri, n. subs). ........-..---2----2----+-eeeeeeeeeeseeeeeeeees 492 PU pra url a ea aenees eens see Sees rete ne cee anes wacarter ceca eden eae Maree ees aee 512 Euceratherium collinum (?) Sinelair and Furlong -.....202.2222222.... 512 TESTS OXIME [sputter ec esa Sars Sete Shc EES A PW eo a iB a 514 FSEPETOC ATES Cece ee EE a eR 514 462 University of Califorma Publications in Geology [ Vou. 10 INTRODUCTION The limestone eaves of California have been the object of much fruitful investigation on the part of students of anthropology and palaeontology concerned especially with the search for evidence bear- ing on the problem of early man in America Although up to the present time no indisputable evidences of Pleistocene man have been found in these eaves, there remain for consideration in the anthro- pological sense many important problems relating to the origin, evolution, migrations and habits of the mammals which constituted a part of the environment in which Pleistocene man must have moved if present in this region. In purely palaeontologic studies the cave faunas are of unusual importance, representing as they do an aspect or a zone of mammalian life not preserved in the more common lacustrine, fluviatile and alluvial accumulations. The recognition of contemporaneity of dis- tinet aspects of faunas, each occupying its own particular type of environment in an extensive geographic province, is of great value in such studies. Thus the importance of mammals from deposits such as Potter Creek and Samwel Caves in Shasta County, inhabiting, as they apparently did, a region physiographically distinct from the adjacent Great Valley of California, can hardly be overestimated. The present study of the mammalian fauna from Hawver Cave is in a manner supplementary to the exhaustive investigation of Potter Creek Cave by W. J. Sinclair and the researches of E. L. Furlong on Samwel Cave. Although the material from Hawver Cave is frag- mentary and not so abundant as that from the Shasta deposits, it is unique in the possession of certain forms heretofore unrecorded from Pleistocene caverns of the state. It is great pleasure to acknowledge indebtedness to those connected with the furtherance of this work. The present research owes its origin to the late Dr. J. C. Hawver of Auburn, California, who first brought the eave and its significant fossil contents to the attention of the University of California. Dr. Hawver followed the scientific work with a sympathetie interest and his assiduous prosecution of collecting work made possible the assembling of a good representation of the Pleistocene vertebrates from the cave. This collection was very kindly presented by Dr. Hawver to the Department of Palaeon- tology, University of California, and forms the basis of the following study. 1918] Stock: The Pleistocene Fauna of Hawver Cave 463 The investigation of the mammalian remains has been made under the supervision of Professor John C. Merriam, to whom the writer is obligated for much counsel and advice. In comparing the Pleistocene remains with Recent forms, the collections of mammals in the Cali- fornia Museum of Vertebrate Zoology were freely drawn upon, and the writer wishes to express thanks to Director Joseph Grinnell and other members of the staff for many courtesies extended during the progress of the work. During early stages of the research, the writer visited Hawver Cave and explored the cavern under the guidance of the late Dr. Hawver. While the work was in course of completion, a second examination of the cave was made. During the last visit the writer was very cordially received and much valuable aid was rendered him by the Pacific Portland Cement Company. ‘The limestone quarry now being operated by this company is situated along the Middle Fork of the American River not far from Hawver Cave. Grateful acknowledgment for much kindness is given to M. J. Johnsson, super- intendent of the quarry. All the text-figures of this paper have been prepared by Mrs. Louise Nash. HISTORY OF PREVIOUS INVESTIGATIONS Originally discovered in the early eighties when the region was actively quarried for limestone, Hawver Cave was subsequently brought to the attention of the University of California by the late Dr. J. C. Hawver of Auburn, California. In 1907, E. L. Furlong? reported on a reconnaissance of the cave, naming the deposit in recognition of Dr. Hawver’s energetic exploration of the cavern and removal of the fossil remains. Furlong’s studies were curtailed by the rise of the water level in the cave, which prevented the removal of much material. The preliminary report of Furlong includes, therefore, only a provisional list of the mammals found. As a result of subsequent excavation by Dr. Hawver much addi- tional material was removed. This is now in the palaeontological collections of the University of California. In 1909, Professor John C. Merriam? discussed briefly the occurrence of human remains in Hawver Cave. Later N. C. Nelson, then connected with the Anthro- 1 Furlong, E. L., Reconnaissance of a recently discovered Quaternary cave deposit near Auburn, California, Science, n.s., vol. 25, pp. 392-394, 1907. 2 Merriam, J. C., Note on the occurrence of human remains in California caves, Science, n.s., vol. 30, pp. 531-532, 1909. 464 University of California Publications in Geology [ Vou. 10 pological department, University of California, commenced detailed mapping of the various chambers of the cave. The bird remains obtained in the course of excavation of Hawver Cave have been studied by Dr. L. H. Miller,* and the report on these forms included also a short discussion of the occurrence of the vertebrate remains. LOCATION OF HAWVER CAVE Hawver Cave is located in Eldorado County five miles almost due east of Auburn, and is approximately 150 miles to the southeast of Potter Creek Cave and Samwel Cave in Shasta County. It is situated to the south of the Middle Fork of the American River at an elevation of 1300 feet or about 700 feet above the present bed of that stream. The county road which extends from Auburn to Cool and thence to Placerville passes immediately to the southwest of the entrance to the cave. As shown by the areal geology mapped in the Sacramento folio,‘ a narrow strip or lens of limestone, lying within an area of amphi- bolitie schist, extends in a northerly direction from the vicinity of Cool to the Middle Fork of the American River and slightly beyond the north bank of that stream. At the present time this limestone, as exposed on the south bank, is being extensively quarried by the Pacific Portland Cement Company. Indications of earlier operations are still to be seen in the presence of deserted lime-kilns situated close to Hawver Cave. RELATION OF CAVE TO TOPOGRAPHY A noticeable physiographic feature of the Sierran region in the vicinity of Hawver Cave to-day is the remarkably even sky-line, indicative of a former physiographic cycle which plainly marks the 1500-foot elevation. The present bed of the Middle Fork hes approx- imately 900 feet below this level. It is generally assumed that the major cutting of the cafions, characteristic of the principal streams of the Sierra Nevada, such as the American River, was accomplished after the Sierran uplift which produced the eastern fault-scarp, and occurred presumably during early Pleistocene time. Whether or not the his- 3 Miller, L. H., Contributions to avian palaeontology from the Pacific coast of North America. Univ. Calif. Publ., Bull. Dept. Geol., vol. 7, pp. 73-75, 1912. 4U. 5S. Geologic Atlas, Sacramento Folio, no. 5, 1894. 1918] Stock: The Pleistocene Fauna of Hawver Cave 465 tory of canon-cutting of these streams involves certain quiescent periods of such length as to allow extensive terraces to be developed, is a matter which can not be adequately discussed as a result of study of the American River directly east of Auburn and of its course in the vicinity of Hawver Cave. Information relating to this problem ean perhaps be furnished most satisfactorily by an extensive investi- gation of streams composing the western watershed of the Sierra Nevada. It has therefore not been found possible at Hawver Cave to associate the Pleistocene fauna from the cavern with the formation of terraces along the adjacent river, as has been done for Potter Creek Cave on the McCloud River in Shasta County. The present course of the Middle Fork is directly athwart the lens of limestone in which Hawver Cave is situated, and there is no reason for believing that the direction of flow of the stream was materially different during Pleistocene time. Apparently the Amer- ican River must have cut below the old surface, at least to a depth now indicated by the floor of the cave, before extensive leaching of the limestone could have been accomplished. The latter process prob- ably aided the weathering of the limestone, and, due perhaps to a more favorable surface drainage, its results may have been greater in the past. At the present time the limestone is weathered in places on the surface, forming crags and numerous fissures. That such open fissures or chasms were developed in the limestone during the Pleisto- cene, and that large animals either fell or were dragged into them, seems to be indicated by the association of parts of skeletons belonging to individuals of the ground-sloth Nothrotherium. Finally, either the chambers of the cavern were entirely filled with osseous material and debris or, as seems not at all unlikely, their entrances from above were temporarily closed. The present entrance to the cave is approximately on a level with a locally developed flat, the formation of which may have been connected with the sealing of the Pleistocene deposits in the cave. No typical terrace accumulations were observed on the flat and it seems to have been formed as a topo- graphic feature incidental to the erosion accomplished by the Middle Fork and by small tributaries of that branch of the American River. This topographic development may account for the pools of water present in all the principal chambers of Hawver Cave even during the summer months. No noticeable movement was observed in these pools and they probably serve as temporary reservoirs for water which is either slowly seeping to lower levels in the limestone or appearing 466 University of Califorma Publications in Geology [ Vou. 10 on the surface as springs. This water is still at work leaching certain areas of the limestone as well as closing cavities by the deposition of carbonate of lime and by the formation of stalactitic growths. Its work now, however, can only be regarded as a minor process, con- sidered in the light of what it has accomplished in the past; and this appears to be principally due to the location of the cave, situated high and dry, as it were, on a spur whose surface supply of water is speedily carried away through the adjacent small gullies. PRESERVATION OF VERTEBRATE REMAINS The matrix from which many of the bones were obtained, is a cave-breccia. A typical specimen of the deposit consists of a mixture of numerous irregular fragments of limestone, broken pieces of stalac- tite and bone fragments together with a reddish-brown dirt derived from the surface soil. The whole is thoroughly cemented with ecar- bonate of ime. A number of the bones were secured from the cave- breccia with some difficulty, while others were imbedded in a less indurated matrix and were easily removed. The vertebrate material is for the most part fragmentary. There are no complete skulls or skeletons. Occasionally a few parts of a skeleton were directly associated in the same block of breccia and evidently belonged to the same individual. Some of the larger re- mains, such as bones of the ground-sloth, had been subjected to much wear before final entombment, so that recognition of parts is often impossible. All of the larger bones are thoroughly impregnated with carbonate of lime. Mixture of apparently Recent mammalian material with Pleisto- cene fossils has in several instances been noted by the writer. These occurrences are, however, few, and so far as observed they seem to be restricted to the smaller forms. The appearance of the material in question offers in each case sufficient ground for suspicion as to its age. OCCURRENCE OF HUMAN REMAINS The occurrence of remains of man in Hawver Cave was investi- gated by Professor Merriam and by members of the Anthropological. department of the University of California. In a short note Professor Merriam’ makes the following statement concerning the human finds: 5 Merriam, J. C., Note on the occurrence of human remains in California caves, Science, n.s., vol. 30, pp. 531-532, 1909. 1918] Stock: The Pleistocene Fauna of Hawver Cave 467 ...In March, 1908, while attempting to open what Dr. Hawver supposed to be an ancient passageway into the lower cave, a number of human bones were found at a depth of twenty feet below the surface, under a mass of cave earth, fallen rocks and soil, over twelve feet in thickness. The remains lay at the lower end of a passageway which has evidently been closed for a long period. In this case, as in that of Mercer’s Cave, remains of extinct animals undoubtedly of Quaternary age were found near the human bones, but the degree of alteration of the unquestionably Quaternary bones differs from that in the human skeletons. Some of the human bones were embedded in a cemented breccia consisting largely of angular fragments of limestone. So far as examined the bones seem to have lost most of their organic matter. A fairly preserved skull in the collection does not differ strikingly from the crania of the modern California Indians, although no comparative study has yet been made by a specially trained craniologist. It is not possible in the case of the Hawver Cave relics to prove Quaternary age for the human bones. As in the other instances mentioned, the inference is, however, that the date of their entombment preceded the present day by centuries, if not by milleniums. MAMMALIAN FAUNA Of the numerous cave deposits known from California, only three, namely Potter Creek Cave and Samwel Cave in Shasta County and Hawver Cave in Eldorado County, have yielded Pleistocene mam- malian remains in sufficient quantity and completeness to allow of broader faunal studies. The deposits may be ranked in the order named according to actual amount of material secured. Mention could be made of other fissure accumulations from which Pleistocene mammals have been recovered. Mercer’s Cave near the town of Murphys, Calaveras County, has yielded mammalian remains, but the material offers only limited information concerning the fauna which lived in the vicinity of that cave during Pleistocene time. From Hawver Cave twenty-four species of mammals are known as contrasted with thirty-four species from Samwel Cave and forty- six species from Potter Creek Cave. It is not improbable that more intensive study of the fauna from Samwel Cave will reveal a number of additional forms from that deposit. Results of such future studies will be expressed in the establishment of other species and subspecies, but it is less likely that extinet genera will be added. Among the twenty-four species of mammals known from Hawver Cave, the presence of such typical Pleistocene forms as Smilodon(?), Nothrotherium, Mylodon and Euceratherium indicates the Pleistocene age of the deposit. Aside from this, however, the fact that twelve, or half the number of forms present, are extinct, conclusively proves Pleistocene. age for the fauna. The percentage of extinct species from [ Vou. 10 468 University of Califorma Publications in Geology Hawver Cave is relatively greater than the percentage of extinct species from either Samwel Cave or Potter Creek Cave. Furlong believes that the Samwel Cave fauna represents a somewhat later stage of the Pleistocene than does the fauna from Potter Creek Cave. Judging only from a comparison of percentages, it would appear that the Hawver Cave fauna is older than that from Potter Creek Cave. As will be indicated below, this determination of the relative age of Hawver Cave is, however, not compatible with that based upon other lines of evidence. The mammalian faunas from the three principal California caves may be conveniently contrasted in the following lists. or a dagger denotes an extinet subspecies or species. An asterisk A double dagger indicates that the genus is extinct. HAWVER CAVE Scapanus, possibly n. sp. Ursus, sp. ~Canis, near dirus Leidy Canis ochropus Eschscholtz Procyon psora Gray Mephitis occidentalis Baird tSmilodon(?), sp. 7Felis hawveri, n. sp. yFelis, probably n. sp. Peromyscus boylei (Baird) Neotoma fuscipes Baird Microtus, sp. Thomomys, sp. ?Aplodontia, sp. Citellus beecheyi (Richardson) yLepus, probably n. sp. tMylodon harlani Owen tMegalonyx(?), sp. tNothrotherium shastense hawveri, n. subsp. Odocoileus, sp. tEuceratherium collinum (?) Sinelair and Furlong 7Bison, sp. yEquus, sp. $Mammut (tooth fragment) PorrerR CREEK CAVE‘ Scapanus latimanus (Bachman) Antrozous pallidus pacificus Merriam, (On isl tArctotherium simum Cope y+Ursus, n. sp. 1 Revised list. yCanis dirus Leidy Vulpes cascadensis Merriam, C. H. Urocyon cinereoargenteus townsendi Merriam, C. H. Bassarisecus astutus raptor (Baird) Mustela arizonensis (Mearns) ySpilogale, n. sp. Mephitis occidentalis Baird Taxidea, n. sp.(?) yFelis, probably n. sp. yFelis, n.sp. Lynx fasciatus Rafinesque Lynx fasciatus, n. subsp. (?) Neotoma cinerea occidentalis Baird Microtus californicus (Peale) yThomomys microdon Sinclair Thomomys leucodon Merriam, C. H. *Aplodontia californica fossilis Sinclair Marmota flaviventer (Audubon and Bachman ) Citellus beecheyi douglasi (Richardson) Eutamias, sp. Callospermophilus chrysodeirus (Mer- riam, C. H.) Sciurus douglasi albolimbatus Allen Sciuropterus alpinus klamathensis Mer- ~ riam, C. H. Sylvilagus auduboni (Baird) tNothrotherium shastense Sinclair tMegalonyx wheatleyi(?) Cope tMegalonyx jeffersoni(?) (Desmarest) tMegalonyx, n. sp. tMegalonyx, sp. t{Camelid 1918] 7Bison, sp. Odocoileus, sp. a Odocoileus, sp. b + tEuceratherium collinum Sinclair and Furlong Oreamnos americanus (Ord) ;Platygonus(?), sp. yEquus occidentalis Leidy 7Equus pacificus Leidy tMammut americanum (Kerr) yElephas primigenius Blumenbach SAMWEL CAVE* Ursus americanus Pallas 7 Ursus, n. sp. Ursus, sp. Vulpes, sp. Urocyon cinereoargenteus townsendi Merriam, C. H. Procyon, near lotor (Linnaeus) Mustela arizonensis (Mearns) Mustela, sp. Mephitis occidentalis Baird yFelis, probably n. sp. Peromyscus maniculatus gambeli (Baird) Neotoma cinerea occidentalis Baird Stock: The Pleistocene Fauna of Hawver Cave 469 Microtus ealifornicus (Peale) ;+Thomomys microdon Sinclair Thomomys leucodon Merriam, C. H. Erethizon epixanthum Brandt *Aplodontia californica fossilis Sinclair Citellus beecheyi douglasi (Richardson ) Callospermophilus chrysodeirus (Mer- riam, C. H.) *Sciurus griseus fossilis Kellogg Sciurus douglasi albolimbatus Allen Sciuropterus alpinus klamathensis Mer- riam, C. H. Castor subauratus Taylor Lepus washingtoni klamathensis Mer- riam, C. H. Sylvilagus auduboni (Baird) tNothrotherium shastense Sinclair tNothrotherium, sp. ¢Megalonyx, sp. Odocoileus, sp. a Odocoileus, sp. b tEuceratherium collinum Sinclair and Furlong tPreptoceras sinclairi Furlong Oreamnos, sp. yEquus occidentalis Leidy 7Elephas, sp. COMPARISON OF CALIFORNIA CAVE FAUNAS Examining the faunas from the three caves as given in the foregoing lists we note the presence of ten distinct, or tentatively determined, genera which are extinct. These are distributed in each of the three deposits, as indicated in the following table: Extinct Genus Arctotherium Smilodon( ?) Nothrotherium Megalonyx Mylodon @eym li Ci eeeee: coereeee cet scapes scoters Euceratherium Preptoceras Platygonus(?) Mammut Potter Creek Hawver Samwel Cave Cave Cave x = & 4 x < x x(?) x Been x x Sen) Oe (2) x x 4 4 As is shown in the above table, Potter Creek Cave possesses the greatest number of extinct genera, namely seven. 2 Partially revised list. Hawver Cave Revision of rodents according to Louise Kellogg, Pleistocene rodents of California, Univ. Calif. Publ. Bull. Dept. Geol., vol. 7, pp. 151-168, 1912. 470 University of Californa Publications in Geology [ Vou. 10 follows next with six genera, while four extinct genera are known from Samwel Cave. Of the total number of extinct genera, three are common to the three caves. These are Nothrotherium, Megalonyx and Euceratherium. It should be noted here that the latter are types not usually associated with a typical plains fauna of the Pleistocene. In the absence of aretotheres, camels and pecearies, the Hawver Cave fauna is more like that of Samwel Cave than like that of Potter Creek Cave, while in the absence of Preptoceras and the presence of a mastodon, it resembles more the fauna from the latter deposit. In this list we note also the presence of two forms, the ground-sloth Mylodon and a sabre-tooth tiger, which are new to the cave deposits of California. Other comparisons of faunas from the Pleistocene caves should also be reported. The true bears probably occur at Hawver Cave, and are known from Potter Creek Cave and Samwel Cave. An extinct species of puma, related to the Recent Felis oregonensis hippolestes, occurs in all three deposits. The large, dire.wolf, known by such abun- dant material at Rancho La Brea, is present in Potter Creek Cave, but absent from Samwel Cave. . csccctceet oon ae ceaat owe ecncan oat eneests its bo tae eect ae nes rr ~10c — +. “eect Observations on the Mode of Accumulation of the Pleistocene Bone Deposits ai of Kancho La Brea, by Reginald C. Stomer 2-5. -.-f...c.scccceacpetcees ong eee 10¢ 554 2) Prelim nary Report on the Horses of Rancho La Brea, by John C. Merriam sss... 20¢ 22. No os ichitheriine Horses from the Tertiary of the Great Basin Area, by John C. PRAT A oan ocanhabococsuaccccnetensetesesutmaztclebdseconsicas once Ines, ase Rese ee ee BS Nace S:opgensamia Horses from Tertiary Beds on the Western Border of the Mahaves Desert,-by John C., Merriam: .22...2ic.-<-ncisashesoceons-gueceescseucedenessuensebusecol eee 24, Pleistocene Beds at Manix in the Bastern Mohave Desert Region, by John P. BU WANDA a... scecectegenescncenccsnncenestutcoroccbevsseveecdatuectivadeecepras theca ase ee eet et ae 25. The Problem of Aquatic Adaptation in the Carnivora, as Illustrated in the Oates ology and Evolution of the Sea-Otter, by Walter P. Taylor ......0.:..-..sesecccssescssseensesee 3 UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 25, pp. 517-521 September 4, 1918 EVIDENCE OF MAMMALIAN PALAEONTOLOGY RELATING TO THE AGE OF LAKE LAHONTAN’ BY JOHN C. MERRIAM Considering the importance of the deposits of Lake Lahontan in Pleistocene history of North America, it is surprising that exceedingly little palaeontologie evidence as to age of these beds has been ob- tained up to the present time. The mammal material available to Russell? in the course of his exhaustive study of these deposits con- sisted of a very few specimens representing four forms, for only one of which a specific determination has been suggested. The remains known to Russell represented an elephant, a horse, a bison, and a camel. A spearhead, found embedded in strata presumed to be of Lahontan age, was also reported. All of the forms known from the Lahontan were assumed to occur in the upper portion of the lake beds series and to have been buried subsequent to the ‘‘intermediate stage’’ of Russell. Of greater importance than the scattered mammal bones secured in the Lahontan beds by Russell is a small collection obtained in 1914 by Professor J. C. Jones of the University of Nevada,* from deposits occurring at Astor Pass, four miles west of Pyramid Lake, and con- sidered to represent Lahontan terraces. In the gravels of these de- posits Professor Jones secured remains representing three or four mammals. One species is clearly determinable as Felis atror, the largest known member of the true cat group. A second is a camel near Camelops, not differing noticeably from Camelops hesternus, well 1 Read before the American Geographical Society, at New York City, December 29, 1916. 2 Russell, I. C., U. S. Geol. Surv. Monographs, vol. 11, p. 238, 1885. 3 See Merriam, J. C., Univ. Calif. Publ. Bull. Dept. Geol., vol. 8, pp. 877-384, 1915. 518 University of California Publications in Geology [Vou.10 known in the Pleistocene deposits of Rancho La Brea. A considerable part of a skull represents a horse, in which the dentition is slightly different from that of the Rancho La Brea Equus occidentalis, and approaches in some respects that of EH. pacificus of the Fossil Lake Pleistocene of eastern Oregon. A single separate upper molar tooth of a horse from the same deposit is nearer in type to FZ. occidentalis. A third important collection representing Pleistocene mammal faunas of the Great Basin province is the material secured by Buwalda‘* in the deposits of Manix Lake, a small body of fresh water which formed in the Mohave Desert region, in Pleistocene time. The Manix collection includes six species of mammals and one or more species of birds, together with four types of fresh-water mollusks. Of these forms the mammals include: (1) a large horse certainly Equus; (2) a somewhat smaller horse; (3) a large camel; (4) a small camel; (5) a fragment representing a proboscidean; (6) an antelope of unknown species. The conditions which governed expansion of the lake in which the Manix deposits were formed resemble in a manner those which con- trolled variation of Lake Lahontan, as described by Russell. It is possible that the climatic changes which influenced Lake Manix are identical with those reflected in Lahontan history, and the Manix fauna may be of the same stage as that of Lahontan. A fourth Pleistocene fauna from the Great Basin provinee is that of Fossil Lake in eastern Oregon, obtained in sandy deposits, the strati- graphic relations of which are not satisfactorily deseribed. There has been some mingling of Recent and Pleistocene remains in the lists of material secured from this locality ; but after all necessary subtractions are made, one of the most important Pleistocene mammal and bird faunas of America remains, including a large number of mammals and over fifty species of birds. Evidence as to the age of the Fossil Lake fauna is to a certain extent contradictory. According to Gilbert® and to Russell, the stage of accumulation of the Fossil Lake deposits is approximately that of Lake Lahontan and Lake Bonneville. Gilbert considered that the highest level of Lake Bonneville corresponded approximately to the last stage of advance of the Wasatch glacier. Similar evidence seems to be furnished by the relation of the highest level of Pleistocene Lake 4Buwalda, J. P., Univ. Calif. Publ. Bull. Dept. Geol., vol. 7, pp. 443-464, 1914. : 5 Gilbert, G. K., U. S. Geol. Surv. Monographs, vol. 1, p. 395, 1890; Russell, I. C., op. cit., vol. 11, 1885. 1918] Merriam: Age of Lake Lahontan 519 Mono to the lowest moraines of the glacier on the east side of the Sierras. If these suggestions are approximately correct, the last stage of Lahontan and Bonneville, approximating the stage of Fossil Lake, would perhaps correspond to the Wisconsin or last glacial epoch. In his study of Lake Bonneville, Gilbert gave particular attention to the problem of age determination of the deposits and made careful comparison of the sediments of the Bonneville and Lahontan stage with those of Fossil Lake in south central Oregon. He considered that in the Fossil Lake region, ‘‘just as in the Bonneville and Lahontan basins, the physical relations indicate that the shore lines and lacus- trine sediments are co-ordinate products of the same expansion of lake waters.’’ He stated further that ‘‘each of the old lakes thus demon- strated stands witness to climatic oscillation, and their geographic relations leave no room for question that they pertain to the same climatic oscillation, and therefore have the same date.’’ The evidence of faunas as interpreted by Osborn and by Hay would fix the age of the Fossil Lake deposits as early Pleistocene. In this palaeontologic determination one of the most important arguments is the absence of bison remains from these deposits, which were evidently formed in an open plains region where bison would be expected to occur. This peculiarity is offset to some extent by the fact that the large wolves of the Fossil Lake beds seem to be exclusively of the modern timber wolf type. The great dire wolf, Aenocyon dirus, has not been recognized in the Fossil Lake fauna, although it is exceedingly abundant at Rancho La Brea and seems to be represented at Potter Creek Cave. Difference in the types of wolves might be due to the northern origin of the modern timber wolf, and to its restriction throughout Pleistocene time to the northern portion of the West Coast region. Within historic time the timber wolf has not been known in middle and southern California. This would not, however, account for its failure to overlap in range with Aenocyon dirus in the Great Plains region. Of the total Fossil Lake fauna 66 per cent of the mam- mals and 34 per cent of the birds are extinct. These percentages are probably not finally determinative of age, but they suggest a stage comparable to that of Hay Springs or Rancho La Brea and earlier than Conard Fissure or Samwel Cave. Compared with the Rancho La Brea fauna that of Fossil Lake is characterized by absence of Bison, which are abundant at Rancho La Brea, and were evidently late arrivals in America. This peculiarity is balanced by absence of the small antelope,-Capromeryx, and the 520 University of California Publications in Geology — [Vou. 10 imperial elephant, early types characteristic of Rancho La Brea. Equus pacificus, the common horse of Fossil Lake, is apparently a more specialized form than FE. occidentalis of Rancho La Brea, and the prong-horn Antilocapra represented at Fossil Lake is apparently a specialized descendant derived from a stock near the Rancho La Brea Capromeryx. It may be that the Fossil Lake assemblage is not older than that of Rancho La Brea, but is merely a contemporaneous northern phase of the same fauna. The absence of bison from the Fossil Lake fauna may be sufficient warrant for considering it older than the upper Lahontan stage, but this item may not be of greater value in separating the time of depo- sition of the two sets of deposits than is the physical evidence used by Gilbert to prove their contemporaneity. If Gilbert is correct in his correlation of Fossil Lake with Lahontan and Bonneville, the Lahontan fauna belongs to a time separated from the present by a period of widespread extinction of organic types and by evolution or introduction by migration of an almost entirely new mammal series, as two-thirds of the Fossil Lake mammal species are extinct and the stage as a whole does not appear like the latest Pleistocene. In some respect the closest resemblance of the few mammal frag- ments from the Lahontan is to the fauna of Rancho La Brea. Of the known Lahontan fauna—Llephas columbi?, Equus near pacificus, Equus near occidentalis, Bison, sp., Camelops, sp., Felis atrox—all of the forms so far as known, with the exception of the horse near E. pacificus, are found at Rancho La Brea. It seems possible that the Lahontan fauna may be representative of a period including the Fossil Lake and Rancho La Brea stages. On this basis it would appear that, whatever the more exact correlation, the Lahontan stage represents a time when the life of this region and that of North America in general was made up of mammal types of which from 60 per cent to 70 per cent have since become extinct and are replaced by new types. We are not of course able to make an exact correlation for the whole of North America in Pleistocene time, but we know that many of the types included in the Rancho La Brea and Fossil Lake assem- blages had a very wide geographic distribution, and it seems that a change such as has occurred since Rancho La Brea and Fossil Lake time is typical of a faunal change over a large part of America. That an extinction of 66 per cent of the mammals in any fauna might occur in a very short time one might readily grant, but the 1918 ] Merriam: Age of Lake Lahontan 521 origin of the new fauna replacing it is not so readily conceived. We may, I believe, assume that the existing fauna of the Lahontan region is not merely a reminder from a large Pleistocene fauna. The origin of the present fauna is not to be accounted for in this manner more easily than one would account for the origin of the existing earth fauna as a remainder from a Mesozoic life series gradually dimin- ishing from period to period. The present fauna is to be accounted for in some part as a remainder and in part as a new development either out of ancestral American forms or out of immigrants from other regions. One might, of course, assume that the existing faunal types arose very recently as mutants developing in response to some great shock given by a physical change such as a great modification of climate, but no evidence has been advanced indicating that such change has ever taken place within a short time measured in terms of years. The rate of change of faunas is fairly known in relation to rate of sedimentation, and there seems to be on record no case in which such an extreme modification of life as is noted between the Rancho La Brea stage and the present has taken place in less than a considerable period measured in terms of deposition. If we assume that the present fauna peopled America by migration, we encounter an obstacle no less difficult to overcome than that pre- sented by rapid evolution without change of geographic situation, as migration from any other continent involves the crossing of great barriers of topography, and belts of varying temperature at least as important as hindrances to migration as are those of relief. Such migration as would be required presumably involves nothing less than general specific change of the migrating types, and a biological reor- ganization process which would take place slowly in the extension of the group by migration transverse to physical barriers. The problem of fixing the date of the Lahontan fauna seems the same as that for other Pleistocene faunas containing a large percent- age of extinct forms. An interpretation of the history of the Lahontan region as shorter than that commonly accepted, which measures the time in long periods expressed in terms of years, involves explanation of the extinction of a great variety of forms over a wide area, and appears to require the relatively sudden repeopling of this area either by more rapid evolution than we have reason to consider probable, or by a more rapid migration across barriers of temperature or of topography than we have reason to beheve could oceur without evo- lutionary changes in the migrating fauna. i : iY 7 ‘ (aul vay bei Satin a as | 7 ‘ 1 1 tt bt : ; 530, 5 textgures isis Mi ae tdnag et eo apie aS Gc Me EPL, pr he ABP 20g hee ook 2 text- figures ye: MAMMALIA FROM THE IDAHO EX? FORMATION ey W PUMA. -LIKE CAT FROM RANCHO LA BREA e BY JOHN C. MERRIAM UNIVERSITY OF CALIFORNIA PRESS BERKELEY UNIVERSITY OF CALIFORNIA PUBLI oF: Norrt.—The University of California Publications are offered eations of learned societies and institutions, universities and librari all the publications of the University will be “sent upon request, For sa publications and other information, address the Manager of the ese Department, University Library, Berkeley, California, U. S. A. Otro HaRRASSOWITZ R. Puiepemee & So LEIPZIG BERLIN Agent for the series in American Arch- Agent for the series in Ame aeology and Ethnology, Classical Philology, aeology and Ethnology, Agricultu [ Economics, Education, History, Modern Botany, Geology, Mathematics, Pa Philology, Philosophy, Psychology. Physiology, Zoology, and Memoirs. — Geology.—ANDREW C. LAwson and JOHN C. Merriam, Editors. Price, volumes volumes 8 and following, $5.00. Volumes 1—9 completed; volumes 10 and 11 i Cited as Univ. Calif. Publ. Bull. Dept. Geol. Volume 1, 1893-1896, 435 pp., with 18 plates, price -.........2-.-.-c-scc--cseceeeeseeees = Volume 2, 1896-1902, 457 pp., with 17 plates and 1 map, price ........ Volume 3, 1902-1904, 482 pp., with 51 plates, price ............-..---.-.- Volume 4, 1905-1906, 478 pp., with 51 plates, price ...... Volume 5, 1906-1910, 458. pp., with 42 plates, price -.2.-.-2..--<.--<¢2n00-s0cere-ensenemenes Volume 6, 1910-1911, 454 pp., with 43 plates, price a A list of titles in volumes 1 to 6 will be sent upon request. ; VOLUME 7 s 1, The Minerals of Tonopah, Nevada, by Arthur S. Eakle .....-.c:ccccccesccssccsseswei Bi 0 2. Pseudostratification in Santa Barbara County, California, by George Davis Loude ; aspen, Discoveries of Caruivora in the Pleistoeane of Ranchos Grea. ae 4. the Nevceve Section at Rirker Pass on the North Side of Mount Diablo, by Bruce : TIE asnsnn-sae adeno ntcoenceebcasnencsoctectacduesrasicbonee ra te, sont ORE SR 5. Contributions to Avian Palaeontology from the Pacific Coast of North America, by Toye Holmes Miller. icc.c sauce tices wea nce cte ne nn pov ates eae sae oe an ee 6. Physiography and Structure of the Western El Paso Kange and the Southern Si Nevada, by. Charles Laurence Baker, -20...cc--2/-c2-2--s-sesecnesponects asnees -ansen coos cee eee . Fauna from the Type Locality of the Monterey Series in California, by Bruce Marti . Pleistocene Rodents of California, by Louise Kellogg ......22..--:--cescceeceeeccetereenerseeveen Tapir Remains from Late Cenozoic Beds of the Pacific Coast Region, by Join Merete ©. stpecss a saat can scat gettecede antec sphecton ech iesag eee ee 10. The Monterey Series in California, by George Davis Louderback e 11. Supplementary Notes on Fossil Sharks, by David Starr Jordan and Carl Hugh Beal .. — 12. Fauna of the Eocene at Marysville Buttes, California, by Roy E. Dickerson ........ 13. Notes on Seutella norrisi and Seutaster andersoni, by Robert w. Pack : 14. The Skull and Dentition of a Camel from the Pleistocene of Rancho La Brea, John .C. Merriam 222-2... 32-212 iorseneecee tee ee 15. The Petrographie Designation of Alluvial Fan Formations, by Andrew C. Laws . “16. A Peculiar Horn or Antler from the Mohave ae of California, by John GC. Mer. on 17. Nothrotherium and Megalonyx from the Picistoomne of Southers Califo ja, | ASHES fer FOGG onan a aoa Sane en rap na tan nn eee rapes eae pce oe Ramee rae eee 18. Notes on the Canid Genus Tephrocyon, by John C, Merriam a 19. Vertebrate Fauna of the Orindan and Siestan Beds in Middle California, by Bs ~ of Rancho Th es by Reginald-C. Stoner 22.2 eee 21. Preliminary Report on the Horses of Rancho La Brea, by John C. Marricat soir 22. New Anchitheriine Horses from the Tertiary of the Great Basin Area, by John Merriam 22 eon atc on cals snecntcecneteee te og eee are eae a > 23. New Protohippine Horses from Tertiary Beds on the redhat Barden of th Mol é Desert; by John C. Merriam! =... 55s) 2 ree : 24. Pleistocene Beds at Manix in the Eastern Mohave Desert Region, | A 536) 721 (6 F: een eee Rat ee Miaenioen i EM re Buenen Se RSA SS ae aE 25. The Problem‘of Aquatic Adaptation in the Carnivora, as Illustrated in the | ) : ology and Evolution of the Sea-Otter, by Walter P. Taylor .. Eoansndusscmr saeco F UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 26, pp. 523-530, 5 text-figures April 20, 1918 NEW MAMMALIA FROM THE IDAHO FORMATION'* BY JOHN C. MERRIAM CONTENTS PAGE Warr Geeta, tes a ee oe 523 Wischiymostailus)?e 1d AWOCNSIS,. MSPs sa c-ce-ncens-ncoe~ feces cee ntes sce teecstceecsesesecenetsedeeccncessenenssaencneee OU IN(eOUnaACOCenUSP lim ere) UW. SPs -scessscs.2-csssectassctecessstetesanstcapecsen teen dedeecndenstanecereroraece 526 BIS; USI) GL DAO CNISUS MTs STO Soe sates ce caret! uted a. reach se aeavyaebneSeccstesdesvasvavwesdaterg Custencetcuddetcecenes 527 INTRODUCTION In attempting to work out a correlation scheme of the Cenozoie formations in the Great Basin region, the writer has found the Idaho formation particularly difficult to interpret with regard to its strati- graphic relations and to its fauna. In the summer of 1916 the prin- cipal exposures in southwestern Idaho were visited in company with Dr. J. P. Buwalda in the interests of the United States Geological Survey. In the course of this investigation a number of significant collections of mammalian remains were obtained. In the material secured there are a few new forms to which it is necessary to make reference in several papers discussing phases of the Idaho problem. A full discussion of the Idaho fauna with particular reference to its affinities will be presented in a later paper. 1 Published by permission of the Director of the United States Geological Survey. 524 University of California Publications in Geology [Vou.10 ISCHYROSMILUS?2 IDAHOENSIS, n. sp. Type specimen, no. 22343, from beds referred to the Idaho formation at locality 3036C, near Froman Ferry on the Snake River in southwestern Idaho. The type consists of the anterior two-thirds of the left ramus of a mandible with the roots of all of the teeth. Specimen no, 228438 (fig. 1) represents a very large sabre-tooth approximating the dimensions of the largest individuals of Smilodon californicus from Rancho La Brea. The Idaho specimen differs from the typical S. californicus in dentition by the presence of a small P3. This tooth is found in a small percentage of the Rancho La Brea sabre- tooth specimens, but is normally absent. The Idaho mandible differs Fig. 1. Ischyrosmilus? idahoensis, n. sp. Outer and superior views of man- dible. Type specimen, no, 22343, % 1%. From beds referred to Idaho formation, near Froman Ferry, Idaho. from that of S. californicus very decidedly in the size and proportions of the flange below the diastema. In S. californicus the flange is com- paratively short, ending posteriorly rather abruptly some distance in front of P;. In no 22348 the posterior end of the flange fades out below the anterior end of P;. A flange of the type seen in the Idaho specimen is found also in Jschyrosmilus ischyrus of the Tulare Pliocene 2 Ischyrosmilus, new genus, founded upon Machaerodus? ischyrus Merriam. Genus characterized as follows: mandible massive; flange clearly marked, relatively wide anteroposteriorly, slightly wider than in Smilodon, not as strongly developed as in Machaerodus ; diastema much as in Machaerodus but shorter than in Smilodon. Pz very small with one root. P; with single posterior cusp or incipient division of this cusp. For more extended discussion, see Merriam, J. C., Tertiary Mammalian Faunas of the Mohave Desert Region, Univ. Calif. Publ., Bull. Dept. Geol., in press. 1918] Merriam: New Mammalia from the Idaho Formation 525 of California, in J. osborni of the Ricardo Pliocene, and in Machae- rodus palacindicus of the upper Siwalik beds of India. The Idaho specimen possesses three mental foramina in contrast to the one large foramen seen in Snvilodon californicus. The tooth crowns in no. 22343 are unfortunately all broken away with the exception of a considerable part of the lower canine and about one-half of the crown of P;. Sufficient portions of the roots remain to give an estimate of the relative dimensions of the teeth. These measurements indicate that P; is relatively smaller and M,; larger than in S. californicus. As these measurements are based upon the upper portions of the roots or upon the neck of the teeth they are not exactly comparable with the measurements from perfectly preserved crowns of S. californicus, as the lower region of the crowns has a some- what longer anteroposterior diameter than the upper portion of the root or the neck. The incisors of the Idaho form appear somewhat thicker trans- versely than in the typical species of Smilodon from Rancho La Brea. With the fragmentary material available it is impossible to draw very satisfactory conclusions as to the systematic position and age of the Idaho sabre-tooth. The presence of a well developed P; taken with the unusual anteroposterior diameter of the flange and the rela- Figs. 2a to 2c. Neotragocerus lindgreni, n. sp. Horn-core. Type specimen, no. 3941, U.S. Nat. Mus. X 1%. Fig. 2a, median view; fig. 2b, cross-section at middle height; fig. 2c, posterior view. From beds referred to the Idaho forma- tion three miles east of Boise, Idaho. 526 University of Califorma Publications in Geology [Vou. 10 tively large size of M; suggest affinity with the Pliocene genus Ischyro- smilus represented in the Ricardo and in beds referred to the Tulare, of California. Machacrodus palaeindicus of the Siwalik beds differs from all of these forms in possession of a two-rooted P3. While it is true that P; may be well developed in adult individuals of Smilodon californicus as in the Idaho specimen, this occurrence is so exceptional that the chance of having this tooth occur in an isolated individual would be very small. So far as the evidence of this sabre-tooth is concerned, it might be presumed to suggest a somewhat earlier geologic stage than that of S. californicus. It should also be noted that the Idaho form is much larger than the specimens from the Ricardo and the Tulare and might therefore be later than the horizons represented by the Ricardo and Tulare faunas. COMPARATIVE MEASUREMENTS S. Cali- fornicus I. ischyrus I. osborni No. 22180 No. 22343 No. 8140 No. 19476 Rancho Idaho Tulare Ricardo La Brea Height of mandible below anterior end of Pj. 49mm. 41.2 34.7 40.3 Thickness of mandible below anterior end Co 9 Ey ee ee yen SP SII i enc ry ie pe cea 2eia 23 ees 18.3 Height of mandible below anterior end of P3.. 52 41.4 36 37 Length anterior side inferior canine to pos- GET TE SUS) AM er <6 Rie ree eee ee neue 135.2 107 81 134.2 Length anterior side Pz to posterior side fos ees lee RAP loge eh RR Ri Oh Pe se 71.6 GIy eee 65.5 Wem orihiorta ce Sit em a esensee sete cee seneee seater oes ee 46.4 33.5 26.5 51.5 C, anteroposterior diameter ................-..----:.---- 19.2 14.5 al0 16.2 Ee; out exOPOSteLLOn (lame tere crests se eeeess 10 7 a6.4 9.9? P;, anteroposterior diameter ............-..-:---------+ 23.7 20 16.7 25 M;, anteroposterior diameter ...........-...2-----2----- 33.2 28.5 24 30 M;, greatest transverse diameter ...............----- 135) 15 11 15 a, approximate. All measurements of teeth approximate on neck or base of crown. NEOTRAGOCERUS LINDGRENI, n. sp. Type specimen, a horn-core, no. 3941, collection of U. 8. Geological Survey assembled by W. Lindgren. Found three miles east of Boise, Idaho, by Edward S. White. Occurrence doubtfully in Idaho beds. The horn-core (figs. 2a to 2c) obtained by Lindgren from the Boise region represents an antelope of the Tragocerus type and ap- proaching the characters of the Snake Creek Pliocene form described as Neotragocerus improvisus by Matthew and Cook.’ 3 Matthew, W. D., and Cook, H. J., Bull. Amer. Mus. Nat. Hist., vol. 26, p- 413, 1909. 1918] Merriam: New Mammalia from the Idaho Formation 527 ’ The Idaho specimen is more slender than N. improvisus, and may show slightly greater lateral compression. It is also more slender, ‘longer and more distinctly flattened transversely than horn-cores of the Recent mountain goat, Oreamnos. Additional material will be re- quired before the position of the species represented by this specimen ean be clearly determined. EQUUS IDAHOENSIS, n. sp. Type specimen, an upper cheek-tooth, no. 22348, from locality 3036C in beds referred to the Idaho formation near Froman Ferry on the Snake River, eight miles southwest of Caldwell, Idaho. Referred to this species is also a lower premolar, no. 22347, from beds referred to the Idaho formation at Froman Ferry. Cheek-teeth large and heavily cemented, characters as in typical Hquus, excepting in the nature of the protocone of the upper cheek-teeth and of the inner gutter between metaconid and metastyld columns of the lower cheek- teeth. Protocone very short anteroposteriorly but distinctly concave on the inner border. Character of the protocone approaching that of Mquus stenonis of the European Pliocene. Gutter on inner border of metaconid-metastylid column of lower cheek-teeth narrow and angular as in Pliohippus. Fig. 3. Hquus idahoensis, n. sp. P4, occlusal view. Type specimen, no. 22348, natural size. Krom beds referred to Idaho formation, near Froman Ferry, Snake River, Idaho. An upper tooth, no. 22348, from loeality 3036C in Idaho beds near Froman Ferry on the Snake River represents an animal as large as Equus pacificus or the largest individuals of FE. occidentalis. The crown (fig. 3) is very heavily cemented. Unfortunately it has suffered so much wear that the original length and curvature cannot be esti- mated. The fossettes are very narrow, as might be expected at this stage of wear, and show plications of such extent as to indicate that considerable folding of the walls would be shown at an early or middle stage of wear. The outer styles are strong. The outer walls of proto- cone and paracone are much flattened. The protocone is small and 528 University of Califorma Publications in Geology [Vou.10 short anteroposteriorly, the stage of anteroposterior abbreviation sug- gesting that in Pliohippus. As in Equus, the anterior border of the protocone is prolonged anteriorly much beyond the isthmus, connecting the protocone with the protoconule. The inner border of the proto- ' cone is distinctly concave, as in Equus. The characters of this tooth are those of Equus, with the exception of shortness of the protocone, which suggests Pliohippus. The characters of the anterior and inner borders of this pillar are clearly those of Equus.. Anteroposterior shortness of the protocone occurs in a few species of Hquus, especially the earlier members of the group., An upper cheek-tooth, no. 22346 (fig. 4), was obtained at locality 3039, in bluffs assumed to be Idaho exposed along the north bank of the Payette River, about four and one-half miles southeast of the town of Payette. The anterior portion of the protocone of this speci- men is broken away. The characters of this tooth do not seem in any particular to differ from those of the Equus. The posterior portion of the protocone column is shorter than this region often appears in EHquus, but matches the proportions commonly seen in Equus occidentalis. There is good reason for considering that this tooth represents a typical Hquus species not far removed from £. occidentalis. It differs from average specimens of EH. occidentalis in greater lateral compression of the fossettes, and in the more pro- nounced complication of the enamel borders of the fossettes. A lower premolar, no. 22347 (fig. 5), from locality 3036C in pre- sumed Idaho beds at Froman Ferry represents a large and very ad- vanced horse. The crown is long and heavily cemented ; the outer faces of the protoconid and the hypoconid are flat. The metaconid-meta- stylid column is long anteroposteriorly and the valleys anterior and posterior to this column are narrow transversely. In all these char- acters this tooth distinctly resembles Equus. In a single feature, namely, in the acuteness of the inner fold of the metaconid-metastylid column, this tooth shows resemblance to advanced forms of Pliohippus. In Equus the gutter is commonly broad and flat. Occasionally, how- ever, it may be narrow and the inner end of the fold acute. On the whole this tooth is of the Equus type with only a single suggestion of Pliohippus in its structure. Compared with the teeth of Equus from the Columbia River blufts near Ringold,‘ Washington, upper tooth 22348 is somewhat larger and the protocone is much shorter anteroposteriorly. The upper tooth 4Merriam, J. C., and Buwalda, J. P., Univ. Calif. Publ. Bull. Dept. Geol., vol. 10, p. 256, 1917. 1918] Merriam: New Mammalia from the Idaho Formation 529 from the Idaho beds at locality 3039 is not apparently less Equus-like than the teeth from near Ringold, unless it be in the character of the anterior portion of the protocone, which is unfortunately broken away in the Payette River specimen. The portion of the protocone remain- ing in the Payette River specimen is perhaps a lttle thicker trans- versely than in the Ringold specimen, but a complete protocone might show more advanced lateral compression. Fig. 4. Hquus idahoensis? M+?, occlusal and outer views, no. 22346, natural size. From beds referred to Idaho formation, bluffs on north side of Payette River about four and one-half miles southeast of Payette, Idaho. Fig. 5. Hquus idahoensis? P3, outer and occlusal views, no. 22347, natural size. From beds referred to Idaho formation, near Froman Ferry, Snake River, Idaho. 530 University of California Publications in Geology [Vou. 10 The lower tooth from locality 3036C from the Snake River is slightly more Phohippus-like than a large lower tooth from the ex- posures near Ringold. In the Idaho specimen the inner faces of the protoconid and hypoconid are a little less flattened, and the inner groove of the metaconid-metastylid column is much narrower and much more acute. In this respect the Idaho specimen is more Pliohippus- like than that from the beds near Ringold. A number of specimens representing foot-bones of a large horse from beds referred to the Idaho show no evident characters distinguish- ing them from the corresponding elements of Pleistocene species of Equus. COMPARATIVE MEASUREMENTS Large Individuals E.idaho- E. idaho- ensis ensis ? KW. occi- E. paci- Nee) M1? dentalis ficus No, 22348 No. 22346 i283 Pt Amteroposterlor (ameter (te csscs.-c-ccceceeeee case 35.5mm. 33 34 34.5 rane verses (Mamet Gr setscc.s.2etscceens <2eeekreeeee ene 34.8 30.6 28.7 32.5 leighton Cro wins ence eee ene renee eee ees see 24.7 B81 ta fc aes No. 22347 sr Pj Anteroposterior diameter ... 5 re S400 gees MTATISVETS GCA Tet Cie eeerncesan: sceseeeseseeeeeenennccreens aS. Sin eee LSS ie Anteroposterior diameter of metaconid-meta- phy Wi(@ (oe) 08 ey Pee rrr eee 5 ea er Tee Te esifel oth One CHOW ANN setae eae See ee Ye Bees UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 10, No. 27, pp. 531-533 April 20, 1918 NOTE ON THE SYSTEMATIC POSITION OF THE WOLVES OF THE CANIS DIRUS GROUP’ BY JOHN C. MERRIAM In a study of the Pleistocene canid fauna of Rancho La Brea the writer had occasion some years ago to consider division of the wolf group into several subgenera. The principal evidence favoring split- ting of the group was found in the wide difference between the dire wolf, Canis dirus, and all other representatives of the Canidae in North America. The only circumstance which prevented setting the wolves of the C. dirus group aside as a distinct genus or subgenus was the lack of such differentiation within this group as is to be ex- pected in a generic division showing as wide a geographic range as that of the C. dirus forms. The suggestion was made that differen- tiation comparable to that characteristic of a genus was perhaps offered by the presence in the Rancho La Brea fauna of a second species of the C. dirus group, namely Canis millert. The millert form was described as a distinct species having characters approximating more closely to those of C. dirus than to the characters of the timber wolves of the C. occidentalis group. Subdivision of the Canis group of America has already been pro- posed by other authors who would separate such distinet groups as the timber wolves and coyotes. Regardless of the question as to gen- eric or subgeneric rank of these divisions, there seems to the writer no question concerning the necessity of this grouping in order to ex- press the relationships and history of these forms. The writer’s view concerning the generic distinction of the wolves of the C. dirus group has received substantial confirmation through 1 Read at eighth annual meeting of the Pacific Section of the Paleontological Society, Stanford University, April 6, 1917. ry Dae University of Califorma Publications in Geology [Vou.10 the discovery of new material representing a wolf related to C. dirus in the Pleistocene of Florida. In his important paper on ‘‘Human Remains and Associated Fossils from the Pleistocene of Florida’’ Dr. E. H. Sellards? has described the first skull of a member of the dire wolf group found outside the California region. The dentition of Dr. Sellard’s specimen very closely resembles that of the type specimen of C. dirus from Indiana. These characters also fall well within the range of variation of the dire wolves of Rancho La Brea. The greater number of the unusual characters distinguishing the wolves of the dirus group are recognized by Dr. Sellards in his specimen from Vero. The Florida skull is, however, characterized by quite different proportions of the facial region, the nose and the palate being much narrower and more slender, and the premolar teeth more widely spaced than in the Rancho La Brea group. In view of these differences, Dr. Sellards seemed justified in separ- ating the Florida wolf as a new species to which he has given the name Canis ayerst. Considering that the several types included in the dirus group represent at least three quite distinct forms, in all of which there appears a group of common characters sharply distinguished from those of other wolves, there is ample justification for distinguishing this group as a separate genus or subgenus for which the name Aecnocyon® may be apphed. The generic characters of Aenocyon are found in the massiveness of skull and dentition, extreme overhang of the inion, shortness of the basicranial region posterior to the glenoid fossae, massiveness of the upper and lower carnassials, reduction of the hypocone of M2, and probably in characters of the skeleton not as yet available from other material than that obtained at Rancho La Brea. The genus Aenocyon was widely distributed over North America in Pleistocene time. Its range extended from the east to the west coast and from Mexico at least as far north as the upper portion of the Mississippi Valley. Whether its geographic range extended into the Canadian area is as yet uncertain. It is possible that the timber wolves of the Canis occidentalis group occupied the northern portion of the continent contemporaneously with the maximum development of the Aenocyon group in the Sonoran region. The geologic range of Aenocyon is also still to be determined. A somewhat puzzling 2 Sellards, E. H., 8th Ann. Rep. Florida Geol. Surv., pp. 152-57, pls. 24, 30, figs. 1, 3, 1916. 3 Aenos: terrible, dreadful; cyon: wolf. 1918] Merriam: Position of Wolves of the Canus dirus Group 533 feature in the distribution of these wolves is found in their absence from the Pleistocene of Fossil Lake, Oregon. The Fossil Lake deposits contain a large vertebrate fauna representing a wide variety of forms and ranging from the largest to the smallest mammals and birds, and including representation of some of the most delicate osseous struc- tures. Wolf remains are well known in this fauna, including bones of both timber wolves and coyotes, but as yet no representation of Aenocyon has been recognized in the collections from this locality. Had Aenocyon dirus or any other member of the group been present in this region in numbers comparable to those known elsewhere in the Pleistocene it would presumably have left at least some trace of its presence. Its absence may be due to limited northern range, or to depo- sition of the Fossil Lake beds at a period earlier, or perhaps later, than that of Rancho La Brea and of other deposits in which specimens repre- sentative of Aenocyon have been found. The recognized species of Aenocyon are A. dirus, A. milleri, and A. ayerst. Aenocyon dirus* (Leidy) is represented in the Rancho La Brea fauna by a wide variety of forms, but always characterized by large size, massiveness of dentition, relatively great width of palate, and of facial region. Aenocyon ayersi®? (Sellards) is characterized by large size, rela- tively narrowness of facial region compared with A. dirus, massiveness of dentition, and relatively wide spacing of the premolars. Aenocyon milleri® (Merriam) is distinguished in comparison with A. dirus and A. ayerst by smaller size, relatively low sagittal crest, and less prominent inion. The dentition is massive as in the other two forms and the premolars are closely set, as is rather common in A. dirus. 4See Merriam, J. C., 'he Fauna of Rancho La Brea. Part II, Canidae, Mem. Univ. Calif., vol. 1, no. 2, pp. 218-246, 1912. 5 See Sellards, H. H., op. cit. 6 See Merriam, J. C., op. cit. UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol 10, No. 28, pp. 535-537, 2 text-figures April 20, 1918 NEW PUMA-LIKE CAT FROM RANCHO LA BREA BY JOHN C. MERRIAM \ eee Included in a considerable variety of representatives of the Felis group known from Rancho La Brea, there is a large puma-lke cat representing a species distinct from any thus far described from North America. As the description of this species is necessary to certain studies on the Felidae now in progress, it is desirable to present a preliminary description at this time. FELIS DAGGETTI, n. sp. Type specimen, a mandible, no. 21572, from locality 2050, Rancho La Brea, California. The mandible and dentition have approximately the dimensions found in the Recent puma of California, but are distinguished. by unusual massiveness of the cheek-teeth and of the jaw, by unusual width of the angle of the mandible, and by the unusual backward curve or sweep of the coronoid process compared with that in Recent pumas. This species is named in honor of my friend and colleague, Mr. Frank S. Daggett, Director of the Museum of History, Science and Art, of Los Angeles, whose interest and co-operation in study of the Rancho La Brea collections have contributed largely to the effective- ness of monographie studies on this fauna now in progress. The Felis daggett specimens represent an animal equaling or per- haps exceeding in size the largest pumas of the present day. They are apparently to be classed with the puma group rather than with the jaguars, and differ widely from the great cats of the Felis atrox type, with which they were associated. The lower jaw represented in the type specimen differs from that of the pumas of the Felis 536 University of Califorma Publications in Geology [Vou. 10 concolor type in relatively large size and massiveness of the cheek- teeth, in the extreme width of the posterior region of P; and P3, and in the stronger backward curvature of the long coronoid process. From the jaguar specimens available for comparison the type speci- Fig. 1. Felis daggetti, n. sp. Outer view of mandible of the type specimen, no. 21572, K %. From the Pleistocene of Rancho La Brea, California. men differs in the more massive lower cheek-teeth, in the greater width of P; and P , in the relatively shorter anteroposterior diameter of P- ;, and to some extent in the greater degree of backward curvature of the coronoid process. Several mandible specimens from Rancho La Brea show the char- acters of the type specimen of F’. daggetti. Among these is the pos- terior portion of a lower jaw representing the first puma-like form recognized in the Rancho La Brea fauna.* Fig. 2. Felis daggetti, n. sp. Dentition, occlusal view, type specimen, no. 21572, natural size, from the Pleistocene of Rancho La Brea, California. MEASUREMENTS OF NO. 21572, TYPE SPECIMEN Greatest length of mandible from anterior end of symphysis to middle Of posterior: end! Of scomdiyle: levee eee ee ee 145.7 mm. Height of mandible below anterior end of Mj .............22..22:2:::0eeeeeeeeeee 31.5 Height of mandible below anterior end of Pj .....-.--.--2-.2----2-c-c-ce-eeeneteeneneeee 27.6 Thickness of mandible below posterior end of Mj ...........2.....---2---.------ 16.3 _ * Merriam, J. C., Univ. Calif. Publ. Bull. Dept. Geol., vol. 7, pp. 42 and 45, 1912. 1918] Height from lower side of angle to upper side of condyle Anterior side of canine alveolus to posterior end of M; Length of diastema between posterior side of canine alveolus and anterior FSG Shera eh e-em ane cece eet Iz, greatest transverse diameter C, anteroposterior diameter of alveolus P3, anteroposterior diameter M;, M;, M; ) M3, M;, anteroposterior diameter ......... greatest transverse diameter ....... transverse diameter across paraconid anteroposterior diameter of protoconid anteroposterior diameter paraconid Merriam: New Puma-like Cat from Rancho La Brea P3, transverse diameter .............-...-...----- Pa Pe RE eee eee eee eee Pj, anteroposterior diameter Pj, transverse diameter o37 31 mm. 79.5 16. A Proboscidean Tooth from the Truckee Beds of Western Nevada, by John ?, ‘17. Notes on the Copper Ores at Ely, Nevada, by Alfred R. Whitman ....... 19. Tertiary Mammal Beds of Stewart and Ione Valleys Is the Boulder ‘‘Batholith’’ a Laccolith? A Problem in Ore-Genesis, by Andrew ey a aes se eae ee LS a cal ater fons necoh fons a sgcadens deel gcanu szabee eu teasty. Sieaboaibanatees Note on the Faunal Zones of the Tejon Group, by Roy B. Dickerson ose Teeth of a Cestraciont Shark from the Upper Triassic of Nps these Calonns) a TEL TISC.C a! AG es B29 a alee SP fers : . Bird Remains from the Pleistocene of San Pedro, g by I d . Tertiary Echinoids of the Carrizo Creek Region in the Chigeada ‘Desert, Ey William Ss. Ww. Kew wewann ene Anan a nnn sen enn nn aennsnenne aa eee ee nan nee: a nawennannnnnenn : . Fauna of the Martinez Eocene of ‘California, ‘by Roy Ernest Dickerson .. Deseription~ of New Species of Fossil Mollusca from the Tater Mazne Neocene of - California, by Bruce Martin ...... 5 e oY Me . The Fernando Group near Newhall, C rnia, . Ore Deposition in and near Intrusive Rocks by ae Lawson eee ea oeane aera ere ero eer near aecemacae ace ciga seer gto leanaesmoced’ . The Ra rtines Be eon ee and ‘A ceaginted ‘Format ions ‘of ae t x Mountains, by Roy E. Dickerson. ...............----.-- dees _ 12. The Occurrence of Tertiary Mammalian Remains | in Northeastern. ‘Nevada, by John (ora, | WEES PITIE i eR ne ar een te, a westseesenesenes ee uenoes _ 13. Remains of Land Mammals from Marine Tertiary Beds in the | Tejon ‘Hills, Cali- s fornia, by John C. Merriam . ses Bae eae ieee ee 14, The Martinez Eocene and Associated “For ations at “Rock Creel on the Western Border of the Mohave Desert Area, by Roy BE. Dickerson ............2....---. \ _ 15. New Molluscan Species from the Martinez Eocene of Southern “California, b Roy E. Dickerson ....... SSE ee eee nhs bay Ree Seen Buwalda ....... ae --0- 18° Skull and Dentition of the Mylodont Sloths of Rancho La Brea, by Chester ‘aan in ee Central a hy an 1 Pablo~ Group ‘of A John P. Buwalda ..... 20. Tertiary Echinoids from a ES a eee t “ “21. An Oceurrence of Mammalian Remains in a Pleistocene Lake Deposit at Astor Pass, near Pyramid Lake, Nevada, by John C. Merriam ............2-.1--s+--2+0@@eecesceeees The Fauna of the San Pablo Group of Middle California, by Bruce L. Clark... ee Index in press. VOLUME 9 s of the Hipparion Group from the Pacific Coast and Great oe Prov- orth America, by John C. Merriam ............. 1 ce of Oligocene in the Contra Costa Hills of P Middle California, by ‘ ] ers Bir c Se Pe ee RS ee ee ce a ace 9 eee eo en Ere eR ere eer m_the Miocene and Pliccene of California, by Jo 2 Cretaceous and Pees of eon and orezon, by Tee 0. ane ern en enna een n wenn e ene cot wonee s from ree La Brea, by Loye ‘Holmes Miller . autor from the F iessroyene of Bas lee co eed By iyo aes n the Gretacenas ce the oe aa, Mountains of Southern Cali- 1 Leroy Packard ..... = ate Fauna from the Cedar Mountain Region ‘of Western Nevada erriam aemeeee ee eceasnne=m === Lower Pliocene. ‘at “Jacalitos Creek ‘and Waltham Canyon, ‘Fresno tnia, by Jorgen O. Nomland .. iddle and Northern California, y Br ozoic Mactrinae of the Pacifie Coast of ‘North America, and Fauna of the Tejon Hocene of “California, b by. Roy E. Dickersod, 1, Zquus to Pliohippus Suggested by Characters of a New Bneres ne of California, by John C. Merriam iccccccsccsce ssssseeeee 1. The Correlation of the Pre- ne Roeks i: “I SO co oO I} . The Occurrence of Ore on the Limestone . Fauna of the Fernando of Los Angeles, by Clarence eo aos y ‘ . Notes on the Marine Triassic Reptile Fauna of Spitzbergen, by Carl Wi . New Mammalian Faunas from Miocene Sediments near Tehachapi P . An ‘American Pliocene Bear, by John C. Merriam, Chester shee an . Mammalian Remains from the Chanace Formation of the Tejon aus Cz . Mammalian Remains from a Late Tertiary Formation at Ironside, Oregon, 5 . Recent Studies on the Skull and Dentition of Wethvoane from Rancho . Further Observations on the Skull Structure of Mylodont Sloths from . Systematie Position of Several American Tertiary Lagomorphs, . New Fossil Corals from ta Pacific Coast, by Jorgen O. Nomland — . The Etchegoin Pliocene of Middle California, by Jorgen O. Nomland . Age of Strata Referred to the Ellensburg Formation in the White . Structure of the Pes in Mylodon harlani, by Chester Stock -.. . An Extinct Toad from Rancho La Brea, by Charles Lewis Camp ; . Fauna of the Santa Margarita Beds in the North Coalinga Region of : . Minerals Associated with the Crystalline Limestone at Crestmore, R . The Geology and Ore Deposits of the Leona Rhyolite, by Clifton . The Breceias of the Mariposa Formation in the Vicinity of Colfax, C: . Relationships of Plioeene Mammalian Faunas from the Pacifie Coast and ¢ . Anticlines near Sunshine, Park County, Wyoming, by C. L. Moody . The Pleistocene Fauna of Hawver Cave, by Chester Stock -..... 5. Evidence of Mammalian Palaeontology Relating to the Age of be mae . New Mammalia from the Idaho Formation, by John C. Merriam. - Note on the Systematic Position of the Wolves of the Canis Dirus Group, . New Puma-like Cat from Rancho La Brea, by John C. Merriam. . The Franciscan Sandstone, by E. F. Davis -..-.2-.--------2:0seeeeeetees nic csaghes VOLUME Andrew C. Lawson ive a oe Nee oe Umipleby © 220020 2. ea a ee nee ee ee Southern Sierra Nevada, by John P. Buwalda) -.2..scc-. cceccceceeeennee Mood y® :40-2280) i Si Nae a a ee ce ree John ©. Merriam. C. Merriam. 3 Nos, 8-and:9.1n* ohe: cover -222-2.22250 i ee ee by: Chester- Stoel, 20 0e.s 52 0 ee ae ee Brea;) ‘by Chester. Stock =... Sesto ace Dice Benne get OE ae ie a rr Columbia River, by John ©. Merriam and John P. Buwalda -.... Jorgen .0.: Nomland 24.032) Se ee eee California, ‘by “Arthur S.. Waklet:c0 2.250: eis eee ee eee eee Clarence. das Moody. 225-2 oee-2eck late gp ee Provinces of North America, by John C. Merriam PROTO Bic cee cite haan sp Lanta RAE ng SL a ae er Sonn COC» Mermviam 2 oo ee a a ee Merriam, WNos-'26,.27;.and--28:'im one. Cover” 2.2....2s-0. ets ee VOLUME 11 he INDEX* Titles of papers in this volume and names of new species, are printed in a bold-faced type. Acanthina (Monoceras) norna, 309; figure of, 325. Adirondacks, granites in, 11. Aelurodon, 487, 441 Aeluropus, 106. Aenocyon, generic characters, 532; distribution of genus, 532; geologic range undetermined, 532; species recognized, 533 ayersi, 533. dirus, not recognized at Fossil Lake, 519, 533; represented at Potter Creek, 519, and at Rancho La Brea, 519. Age of Strata Referred to the Ellens- burg Formation in the White Bluffs of the Columbia River, 255. Age determination, Lyell percentage method of, 225. Agriotherium (Hyaenarctos), indicates Pliocene rather than Miocene, in Alachua, 441. Ajibik quartzite, 9. Alachua fauna of Florida, 422, 4389, 441, 442; list of, 439. Alaska, ore and garnet zones at White- horse Copper Belt, Yukon, 33. Algoman granitic assemblage, 6, 7, 8, 15 Algonkian, division of pre-Cambrian time, 17; extent of system, 17. Allen, G. M. cited, 276, 278. Allen, R. C. and Barrett, L. P., 3, 4; cited, 9, 10, 14. Alluvium in anticlines, Sunshine, Wy- oming, 455. Ameghino, F., cited, 138, 162. American Pliocene Bear, An, 87; occurence, 88; dentition, 90; skel- etal elements, 97-105; relation- ships, 105. American Pliocene faunas: Pacific Coast, 424; Great Basin, 427; Great Plains, 434; Atlantic, 438; time relations, 439; correlation with Old World Faunas, 442. American Tertiary Lagomorphs, Sys- tematic Position of Several, 179. Americanus-lentiginosus-cognatus groups of North American toads, 289. Amiantis communis, 305; plate show- ing, 315 Amphibian remains in Rancho La Brea, 287. Amphicyon, 100. Anderson, F. M., cited, 46, 193, 194, 207, 223, 294, 295. Anderson, R.., te aot 195, 223, 224, 295, 296, 297, 3 Animikian series, rain by Algo- man granite, 7; absent in Rainy Lake and Steeprock Lake dis- tricts, 8; correlatives of 10, 14. Animikie, use of term, 4. Anodonta, 203. nitida, 231; figure of, 249. Antelope, unknown species, from Manix Lake, 518. Anthony, A. W., information given by, 129 Anthony, H. E., information given by, 129 Anthony, R., cited, 146. Anticlines Near Sunshine, Park County, Wyoming, 445. Antilocapra, represented at Fossil Lake, 520 Apatite, 348. Aphelops, 437. Aplites, 5. Aplodontia californica fossilis, 470. Apophylite, 350. Aragonite, 348. Archean Era, 18. Archaeolagus, 180, 181. ennisianus, figures of, 180, 181. Archeozoie, confusion in use of term, Arctotherium, 87, 88, 90, 95, 96, 98, 102, 104, 106, 107, 108. 109, 471, californicum, 100. simum, 90, 96, 98, 100. Arizona, ‘relationship between ore and garnet zones in: at Washington Camp 26, at Silverbell, 27. Arnold, R., cited, 50, 40, 41, 42, 46, 47, 193, 198, 223, 295, 297, 299, 302. Arsenopyrite, 352. Astor Pass, Nevada, 517. Astoria Oligocene, corals in, 189. Astrangia boreas, 186. grandis, 186. insignifica, 46. Astreopora occidentalis, 187. Atwood, W. A., cited, 405. * Univ. Calif. Publ. Bull. Dept. Geol., vol. 10. Index Augite, 349. Austria, Triassic ichthyosaurians in, 64. Axinite, 350. Bad River, dolomite, 8. Balanophyllia, 189. Barrett, L. P. and Allen, R. C., 3, 4; cited, 9, 10, 14. Barstow, California, 117, 122. Bartsch, P., cited, 40. Batholithic invasion of Seine series, 7. Bear, An American Pliocene, 87; oc- currence, 88; dentition, 90; skeletal elements, 97-105; relationships, 105. Beaver tooth, fossil, from Etchegoin area, 217. Beetles, fossil, Pleistocene, 287. Benton shales, 450; section of forma- tion, 453. Berkeley Hills, rocks of, 364; faulting of, 366. ; Big Blue, The, of the Santa Margarita formation, 295, 297. Bighorn Basin, Wyoming, 445, 447, 456, 458. Big Sandy Creek, California, fauna from, 215. Bijiki iron formation, 10. Biotite, 349. Bird remains in Hawver Cave, 464. Bison, at Hawver Cave, 471, 514; at Lahontan beds, 520; at Rancho La Brea, 519; absent at Fossil Lake, 519. Blainville, H. N. D., cited, 92. Blanco fauna, 434; characteristics of, 435; list of 435. Blastomeryx, 437, 441. Bonneville. See Lake Bonneville. Boreal character of Los Angeles and San Diego faunas, 50. Boreas-canorus group of North Ameri- can toads, 289. Boron, rock element, 350. Borophagus, 435. Borsonia inculta, 54; figures of, 51. Breccias of the Mariposa Formation in the Vicinity of Colfax, California, 383; in other areas, 384; origin of, 384, 406; occurrence, 391; mega- scopic features, 394; boulders in, 396; microscopic features 397; resemblance to tillites, 397, 407, extent of 397-398; structure, 410; illustrations of, 414, 416. Brown, B., cited, 167, 473. Bruce series of pre-Cambrian rocks, 11. Brucite, 331, 332. Buccinidae, 48. Bufo alvarius, 289, 290. boreas 287. boreas, 287, 289, 290. halophilus, 287, 288, 290. Nestor, 287; characters of, 288, 289; figures of skull of, 288; table of measurements of skull, 291, 292. punctatus, 290. woodhousii, 289. Burmeister, H., cited, 169, 280, 281. Butterworth, E. M., 21. Buwalda, J. P., 75, 255; cited, 111, 113, 129, 431, 432. Cache Peak, California, fauna of, 80. Calaveras formation, 386; unconfor- mity with Mariposa formation, 406. Calcite, blue, 334. California, presence of Nothrotherium, 164; map of, showing Pliocene localities, 199; limestone caves of, 462. See also Hawver Cave: Potter Creek Cave; names of for- mations, localities, etc. Calkins, F. C., cited, 257. Camelid, indet., 127. Camelops, 517: at Lahontan beds, 520. hesternus, 517. Camels, from Manix Lake, 518. Camp, C. L., 287. Cancellaria crassa, 237. crawfordiana, 47: figures of, 63. fernandoensis tribulis, 238. quadrata, 56; figures of, 61. rapa, 240; figure of, 253. Canid Pleistocene fauna, 531. Canis ayersi, 532. dirus, 470, 471. near dirus, 478; figures of, 479. milleri, 531. occidentalis, 531. ochropus, 479. pambasileus, 470. Canis Dirus Group, Note on the Systematic Position of the Wolves of, 531. Capromeryx, 519, 520. Carnivora from Hawver Cave, 478. ° Carson City, Nevada, 284. Carrizo Creek, California, Pliocene of, Carter Mountains, Wyoming, 448. Caryophyllia arnoldi, 188. californica, 188. oregonensis, 187. pedroensis, 188. Castro Valley, California, physiog- raphy of, 362. Cave faunas. See Hawver Cave; Potter Creek Cave; Samwel Cave. Catonyx, 275, 283. Cenozoic formations in Great Basin region, 523. Chanac Creek, California, 114. Index Chanac Formation of the Tejon Hills, California, Mammalian Remains from the,111; stratigraphic position, 112-113; lithologie characters of, 114; mode of origin of, 114; list of fauna, 426. See also Mammalian Remains; Tejon Hills. Childs, L. J., cited, 328. China, Schansi fauna of, 442. Chino Hill, California, minerals from, 329-334; analysis of limestone from quarry of, 334; illustration showing, 354. Chione elsmerensis, zone of, 216. semiplicata, 305; plate showing, 317. Choloepus, 146. Chondrodite, California, 333. Se eee dirus meridei, 52; figures WoL Ol: packardi, 235. rectirostris, figure of, 63. Cirripedia supposed radiolites referred to, 41. Clark, B. L., cited, 40, 111, 193, 226, 294, 298, 302. Clark, C. W., 361. Clinochlore, 348. Cloverly formation in anticlines of Sunshine, Wyoming, 450. Coal and carbonaceous deposits in Etchegoin, 207. Coalinga, California, Pliocene section near, 193, 203, 227; faunal zones, 216; occurrence of Etchegoin fauna in, 218, 230; diastropic movements in, 227; palaeon- tology of, 294, 295; geology and oil resources of, 295: figures show- ing sections of, 296, 298. Cobalt, Great Lakesregion, 10; series, 11. Cockerell, T. D. A., cited, 166. Cody formation, shale, in anticlines of Sunshine, Wyoming, 454, 458. Coelodon, 137. Coleman, A. P., cited, 404. Colfax, California, breccias in vicinity of, 383; geologic map of region, opp. 384. See also Breccias; Mariposa formation; ete. Collins, W. H., cited, 2, 10, 13, 14. Columbella (astyris) constantia, 53; figures of, 61. carinata, 47. Comanche Creek, California, 115. Commercial Rock Quarry, Crestmore, California, minerals in, 329, 332- 334, 344, 348 353; plate showing, 356. Conard fissure, 472, 519. Conglomerates, Ogishke, 7; Oakland, 364; classification, 399; fluviatile, 401. Conlin, J. M., acknowledgment of as- sistance, 362. [541] Cook, H. J., cited, 422, 435, 440. Cope, E. D., cited, 180, 181, 431, 434, 473. Copper Bullion Mine, Mackay, Idaho, relations of ore to rocks, 33. Copps formation, 10; correlation with Animikian formation, 14. Corals, species of, in Astoria Oligocene, 9 Corals from the Pacific Coast, New Fossil, 185. Corbula tenuis, 59; figures of, 63. Correlation of the Pre-Cambrian Rocks ofthe Region of the Great Lakes, 1. Crenshaw, J. L., cited, 376. Crepidula, 46. princeps, 46. rugosa, 46. Crestmore (California) limestone for- mation, description of, 328-329; rocks in: intrusive, 329, limestone, 330-331; minerals in: apatite, aragonite, 348, apophyllite, 350; augite, 349, axinite, 350; biotite, 349, blue calcite, 334, brucite, 331, 332, chondrodite, hy clinochlore, 348, crestmoreite, 344, datolite, 350, diopside, 340, epidote 349, feldspars, 349, garnet, 339, gra- phite, 333, hornblende, 349, hydro- magnesite, 339; laumontite, 352, monticellite, 342, okenite, 351, opal, 352, phlogopite, 334, preh- nite, 351, quartz, 350, riversideite, 347, scapolite 350, serpentine, 334, titanite, 349, tourmaline, 350, vesuvianite, 338, wilkeite, 343, wallastonite, 334, xanthophyllite var. waluewite, 341, zircon, 349; sulphide minerals, 352; oxydation products, 353. Crestmore, Riverside County, Calif- ornia, Minerals Associated with the Crystalline Limestone at, 327. Crestmoreite, new mineral, 344-346. Cretaceous system in the anticlines near Sunshine, Wyoming, 450-454. Crystal Falls district, Lake Superior, formations in, 8. Crystalline Limestone at Crestmore, Riverside County, California, Min- erals Associated with the, 327. Cymbospondylus? natans, 66. petrinus, 67. Daggett, F. S., acknowledgment of assistance, 139, 166; species named for, 535. Dakota formation, Wyoming, 450, 458. Dakota sandstone, 451, 454. Dall, W. H., cited, 41, 225, 226. Dames, W, cited, 65. Daonella limestone, 64. Darton, N. H., cited, 447. Index Datolite, 350. Debilis - punctatus - alvarius section of North American toads, 289. Dendrophyllia californiana, 188. hannibali, 188. tejonensis, 188. Dhok Pathan fauna of India, 442. Diabase near Colfax, California, 386. Diablo Range, Etchegoin fauna west of, 214. Dice, L. R., 179; cited, 258, 487. Dickerson, R. E., cited, 294. Dinocyon, 441. Diopside, 340, 341; figures of, opp. 360. Dipoides, 442. Dire wolf, 531, 533. Dollo, L., cited, 66. Dolomite, Bad River, 8; Kona, 8; Randville, 8. Dolores Mine, Mexico, 31. Dosinia jacalitosana, figure of, 25. Dromomeryx, 81, 437, 441. Eakle, A. 8., 327. Edentata from Hawver Cave, 488. Eldridge, G. H., cited, 49, 447. Elephant, imperial, absence of, Fossil Lake, 520. Elephas, 438; absent from Hawver Cave, 470. columbi (?), 520. Ellensburg Formation in the White Bluffs of the Columbia River, Age of Strata Referred to, 255. Elmhurst, California, 363. Emigrant Gap _ anticline, Mowry Shale from, 452. Emmons, W. H., cited, 376, 377. English, W. A., cited, 194, 208, 224. Eocene, Payette, relation of, to Idaho formation, 432. Eparchean Interval, 13, 18. Epidote, 349. Epilaurentian Interval, 13, 18. Epitonium retiporosa, 47, 51; figure of, 61. varicostata, figure of, 253. Equus, 259, 432, 438, 527, 529; present at Hawver Cave, 470; present at Manix Lake, 518. idahoensis, 527; figure of teeth, 529. occidentalis, 518, 520, 527. pacificus, 518, 520, 527. Etchegoin group of Middle California, 197; areal distribution, 197; rela- tion to Santa Margarita formation, 200, 201, 296, 297, to Tulare forma- tion, 202, thickness 203; structure, 205. lithology: sandstone, clay, and con- glomerate 206; coal and carbon- at Wyoming, aceous deposits, 207: rhyolitic tuffs, 208; gypsum, 209; limestone, 210. [542] Fauna: invertebrate, 210; west of Diablo Range, 214; of lacustrine beds, 215; range of temperature and depth, 216; serpula reef, 216; faunal zones, 210, 216, 228, 422, vertebrate, 216; faunal list of ee of Coalinga district, 18. Age and correlation of, 223; history of correlation, 223; age determina- tion, 204, 225; correlation with other Pliocene formations, 226; occurrence of Etchegoin species by localities, 227, 230; description of invertebrate localities, 228: description of species: Anodonta nitida. 231; Cancellaria crassa, 237; fernandoensis tribulis, 238; rapa, 240; Chrysodomus packardi, 235; Fissuridea unica, 234; Macoma inquinata affinis, 233; Murex concinna, 236; tethys, 236; Pecten egregius, 231; P. etchegoini, 239; P. proteus, 232; Semele fausta, 233; Serpula (?), 239; Tegula (Chlorostoma) pulcella, 235; Thracia formosa, 234; Tro- phon belcheri airtum, 237. See also Jacalitos formation. Etchegoin, Lower, 226, 228. See also Jacalitos formation. Etchegoin, Upper, 227, 228. Etchegoin Pliocene of Middle Calif- ornia, The, 191. Etchegoin-Tulare section, 424; list of fauna from, 425. Euceratherium, in Hawver Cave, 467, 470, 474, 513. collinum, 513; teeth, 514. Evidence of Mammalian Palaeontology Relating to the Age of Lake Lahontan, 517. Extinct Toad from Rancho La Brea, An, 287. Fairbanks, H. W., cited, 294, 302. Fanglomerates, 405. Fauna, canid Pleistocene, 531. Fauna of the Fernando of Los Angeles, 39; occurrence, 40; related occur- rences, 40; list of species, 42; general features, 46; compared with related faunas, 48; three faunal horizons, 49; description of species, 51-59. Fauna of Hawver Cave, The Pleis- tocene, 461; remains in, 464; presence of Nothrotherium, 465; preservation of vertebrate and of human remains, 466; mam- malian fauna, 467; list of, 468; comparison with other faunas; California cave, 469, Port Kennedy deposit and Conard Fissure, 472, measurements of Index Rancho La Brea, 474, Recent, 475; ecology, 477; description of material; insectivora, 478, Carni- vora, 478, canidae, 478, Machaero- dontinae, 480, Felinae, 482, Roden- tia, 486, Edentata, 488, Ungulata, 512. Fauna of the Santa Margarita Beds in the North Coalinga Region of California, 293; Arnold’s list of, 299; Nomland’s list of, 300; list from Tejon Hills, 302, from San Luis Quadrangle, 302, at base of “Monterey”’ shale, 303, from the type section, 303, from Salinas Valley, 304; description of species, 305-372. Faunas, cave, of California, 462; extinct genera in, 369-472. See also Hawver Cave; Potter Creek Cave; Samwel Cave. Feldspars, 349. Felinae from Hawver Cave, 482. Felis, 483, 484. atrox, 517, 520. daggetti, 535. hawveri, 482, 483; figure of, 481. oregonensis hippolestes, 470. Felsite facies, Leona rhyolite, 368. Felsophyric facies, Leona rhyolite, 369. Fernando of Los Angeles, Fauna of the, 39. Fisher, C. A., cited 446, 447. Fissuridea unica, 233; figure of, 253. Florida, (Pliocene Alachua) beds of, 226. Fluviatile conglomerates, 401. Fossil Corals from the Pacific Coast, New, 185. Fossil Lake, Oregon, fauna, age of, 518, 519, 520; comparative stage of, 519; bison absent, 519, Antilo- capra, and Equus present, 520; correlation of, with that of Bon- neville and of Lahontan, 520. Fraas, E., cited, 65. Freudenberg, W., cited, 107. Frontier formation, anticlines of Sun- shine, Wyoming, 453; indicative of shallow marine conditions, 458; marks break between Dakota and Mesaverde formations, 458. Furlong, E. L., cited, 513. Fusinus fabulator, 309; figure of, 327. Gabbro, northwest of Colfax, 387. Galena, 353. Garnet, 339; analysis of, 340. Garnet Zones, Occurrence of Ore on the Limestone Side of, 25. Geikie, A., cited, 401. Geology and Ore Deposits of the Leona Rhyolite, 361; physical features of area, 362; pre-Recent erosional sur- face, 363; geological history, 364. Gervais, P., cited, 278, 279. [543] Gester, G. C., cited, 202. Gidley, J. W., cited, 441. Gilbert, G. K., cited, 518. Gilbert, J. Z., cited, 39, 277. Glacial “‘tillite,’’ 402. Glycimeris zone, unconformity above, 196. Gogebic district, Lake Superior, 8. Goodrich quartzite, 10. Gooseberry Creek, Wyoming, “agbistiae 448; relation to older structures, 448; Wasatch beds on, 448. Gooseberry Creek Anticline, Sunshine, Wyoming, position and structure, 457; plates showing, opp. 45 50, 454; figure of section of, foll. 459. Granodiorite, 328, 329, 330; analysis of, 330. Granite assemblages, 6. See also Algoman, and Laurentian granitic assemblages. Granitiec batholiths in post-Keewatin period, 5. Granitic invasions, two periods, 5; date of, 7; chronological equiva- lence on Lake Superior, 9; occur- rence of Temiskamian between, 10; events connected with 12, 13; result of, 12; time required, 12: subdivisions of time, 16. Graphite, 333. Grass Creek, Wyoming, oil-bearing sandstones of, 454. Great Basin Provinces of North America, Relationships of Pliocene Mammalian Faunas from the Pacific Coast and, 421; Pacific Coast province, 424; Great Basin province, 427; Great Plains pro- vince, 484; Atlantic province, 438; Pliocene faunas in, 427, 439; Cenozoic formation in, 523. Great Lakes, Correlation of the Pre- Cambrian Rocks of the Region of the, 1 Great Plains province, 434; tabulation of fauna from, 488. Grenville series, 11. Greybull River, source of, 448; drains anticline area at Sunshine, Wyom- ing, 448; relation to older struc- tures, 448; history of, 449; terraces at junction with Wood River, plate showing, opp. 456. Ground sloths from Santa Cruz, 164, 282, 284, 286. Gunflint Lake, geologic district Great Lakes region, 6. Gypsum in the Etchegoin, 209. Haliotis, 46. Hamlin, H., cited 40, 41. Hanbury slates, 9. Hanford, Washington, Ellensburg ex- posures, 255, 257. in Index Hapalops, compared with Nothro- therium, 140, 142, 149, 502-512, with Mylodon harlani, 275; Noth- rotherium derived from, 162. elongatus, 152. gracilidens, 141. indifferens, 152. longiceps, 141, 145. vulpiceps, 141. Harkness, H. W., cited, 284. Hastings series, correlations of, 14. Hawver, J. C., cited, 462. Hawver Cave, The Pleistocene Fauna of, 461. Hawver Cave, investigations of, 463, location 464, relation to topo- graphy, 464; vertebrate, and human remains in, 466; fauna of, see Fauna of Hawver Cave. Hay, O. P., cited, 160. Hay Springs, age of Fossil Lake fauna in reference to fauna of, 519. Haywards fault (rift), compared with San Andreas fault, 366, 409. Helarctos, 106. Hemibradypus, 146. Hewett, D. F., cited, 447. Hintze, Jr., F. F., cited, 447, 453, 454. Hipparion, 255, 431, 438, 441, 442. anthonyi, 131; figures of, 132. Hore, R. E., cited, 404. Hornblende, 349. Horse remains at Idaho localities, referred to Equus, 432. Hospital Creek, California, 118. Huene, F. von, cited, 71. Human footprints (supposed) in Pleis- tocene strata at Carson City, Nevada, 284. Human remains in Hawver Cave, 463, 466. Huron, Lake. See Lake Huron. Huronian, significance of the term, 4, 16, 17, 18; three divisions of, 5; events occurring between Ontarian and, 17; extent of system, 17. Hyaenarctos, 91, 93, 95, 96, 98, 106, 107, 109, 442. insignis, figure of teeth, 92. paleindicus, 95; figure of tooth, 92. punjabiensis, 95, 107; figures of teeth, 94, 96. sivalensis, figure of tooth, 94. Hydromagnesite, 338. Hyla arenicolor, 289. Hyperleptus, 142. Hypohippus, 81. Hypolagus, 181; dentition, 181. vetus, figures of teeth, 181. Ichthyosaurs, triassic, 63, 64; caudal fin of, 66; in Arctic North America, 72. Idaho, ore and garnet zones, at Seven Devils, 28, at Mackay, 33. [544] Idaho formation, Oregon, fauna -col- lected from by Lindgren, 131, 431, Cope, 431, Merriam and Buwalda, 431, 532; list of fauna referred to, 432; relation to Payette Eocene, 432; age of, 432, 434, 442. Indarctos oregonensis, 87; figures of, 90, 91, 92, 94, 96, 99. salmontanus, 93, 95; figure of tooth, India, Dhok Pathan fauna of, 442. Ingram Creek, California, 120. Inoceramus, casts of, in Frontier for- mation, Sunshine, Wyoming, 457. Insectivora from Hawver Cave, 478. Inter-granitic division of time, 12. International Geological Congress at Toronto, 1. Intrusive rocks in Crestmore formation, 329; minerals associated with, 349. Invertebrate faunas in horizons with vertebrate faunas, 195. Invertebrate zones of Etchegoin, 210, 228, 230. Invertebrates from the “Jacalitos’”’ or Lower Etchegoin, 211. Iron formation, Negaunee, 9; Bijiki, 10. Iron-bearing rocks, Lake Superior, correlated with Animikian, 5. Tronside, Malheur County, Oregon, fossil mammalian beds at, 129, 130. Tronwood iron formation, 9. Ischyrosmilus, 442, 524. idahoensis, figures of, 524. ischyrus, 524. Jacalitos formation, inclusion with Etchegoin, 193, 197; division of Coalinga beds, 295; list of species from, 197; list of invertebrates from, 211. John Day beds, Oregon, 256. Johnson, J., cited, 376. Johnson, H. R., cited, 198. Jones, J. C., cited, 517. Keewatin series segregated from Hur- onian 5; cut by Laurentian, 11. Keweenawan series, Lake Superior, correlation of, 5. Kellogg, Louise, cited, 181, 182, 217, 469. Kettleman Hills, California, Etchegoin material in, 217. Knife Lake slate conglomerate, 7. Knight, C. W., and Miller, W. G., cited, 13, 14, 16. Knopf, A., cited, 398. Kona dolomite, 8. Kreyenhagen Hills, Etchegoin material in, 217. Lacustrine (?) beds, fauna of, 215. Lagomorphs, Systematic Position of Several American Tertiary, 179; new genera of, 180, 181, 182. Index Lake Bonneville, comparative age of fauna, 518, 519, 520. Lake Huron district, sequence of pre- Cambrian rocks in, 10, 11. Lake Lahontan, Evidence of Mam- malian Palaeontology Relating to the Age of, 517. Lake Lahontan deposits, mammalian fauna in, 517, 518, 520; fauna of, compared with those of Fossil Lake, and Rancho La Brea, 518, 519, 520; correspondence in age to Wisconsin epoch, 519; problem of origin of, 521. Lake Manix fauna, 518. Lake Mono, evidence furnished on age of Fossil Lake fauna, 519. Lake Temiskaming district, sequence of pre-Cambrian rocks in, 10. Larsen, E. S., cited, 376. Laumontite, 352. Laurentian, granite assemblage, 6, 7, \ 17; basis for correlation 8; pre- ceded quartizite and dolomite formations, 9, and the Tem- iskamian (Sudbury) series, 10; presence of in southeastern Ont- ario, 11; cuts the Keewatin and Grenville series, 11; correlated with Huronian, 11; petrographic discrimination between Algoman and, 15. Laurentian Revolution, 7. Lawson, A. C., cited, 203, 205, 362, 384, 399. LeConte, J., cited, 284, 285. Leidy, J., cited, 139, 488. Leith, C. K., cited, 14, 15. Leona Chemical Company, 372. Leona Heights, California, rift valley near, 366; faulting at, 366-367; pyrite at, 373; metallographic study of, 374; mineralogy of, 374; genesis of ore of, 375; fracturing of ore of, 377. Leona Heights Mine, 372; figure of plan of, 372. Leona Rhyolite, Geology and Ore Deposits of the, 361. Lepus, genus, 179; probably new species, 487. californicus, 488. campestris, 488. ennisianus, type species of Archae- olagus, 180. vetus, type species of Hypolagus, 181. washingtoni klamathensis, 488. Lestodon, 275; comparison of Mylodon harlani with, 279, 283. armatus, 278. - Lima (L. hamlini), giant found at Los Angles, 41. Limestone, 210, 331; Daonella, 64. See also Ore on the Limestone Side of Garnet Zones. [545] Limestone caves of California, 462. Lindahl, J., cited, 142, 146. Lindgren, W., cited, 377, 398, 411, 412, 431, 526. Lithology, means of correlation of Pliocene deposits of the Etchegoin, 192, 206. Littorina mariana, 203. Logan, Sir Wm., quoted, 10. Lonoak, California, fauna from, 215. Lone Star Quarry, Crestmore, Calif- ornia, 329. Los Angeles, Fauna of the Fernando of 39; Fourth and Fifth street beds, 39, 40; Third street tunnel ma- erlal, 41; correlations of these beds, 42, 47. Los Angeles Museum of History, Science, and Art, 138, 158, 165, 168, 268. Loup River or Nebraska formation, Pliocene types in, 438. Lueas, F. A., cited, 431. Lull, R.8., cited, 268. Lund, P. W., cited, 137. Lupton, C. T., cited, 447, 451. Lydekker,’R.., cited, 107. Lyell percentage method of age deter- mination, 225. McDonell, D. A., acknowledgment to, 362. Mace, C. H., cited, 372. Machaerodontinae from Hawver Cave, 480. Machaerodus palaeindicus, 525. Mackay, Idaho, contact metamorphic copper deposits at, 33. Macoma inquinata affinis, 233; figure of, 249. nasuta, 203. vanvlecki, figure of, 247. Macrocallista densa, 58; figures of, 63. Magnesia, 331. Mammalian Palaeontology Relating to the Age of Lake Lahontan, Evidence of, 517; collections of material; Russell’s, 517. Jones’ collection from Astor Pass, 517, Buwalda’s, from Manix Lake, 518, from Fossil Lake, 518, from Rancho La Brea, 519; comparisons 519-521. Mammalian Remains from the Chanac Formation of the Tejon Hills, California, 111; composition and relationships, 116; description of, 117-127. Mammalian Remains from a Late Tertiary Formation at Ironside, Oregon, 129; occurrence and age of, 130; description of species, 131-135. Mammut form in Hawver Cave, 471. progenium, 441. Index Mangidia muricidea, 55; figures of, 61. Manix Lake, fauna of, 518. Mansfield, G. R., cited, 339, 400. Maragha fauna of Persia, 442. Marine conglomerates, 400. Marine faunas in the Upper Etchegoin, 203. Marine Triassic Reptile Fauna of Spitzbergen, Notes on the, 63; occurrence, 63, 64; Mixosaurus and Phalarodon 65; Pessosaurus and Shastasaurus, 68; Pessopteryx and Omphalosaurus, 69; faunal rela- tionships, 71. Mariposa formation, location and topography, 383-384; geologic map of, opp. 384; geology of, 386; stratigraphy of, 388; slates of, 389; figure showing slaty cleavage, 390; sandstone 390, figure showing, 420; breccia, 391-397; fauna of, 398; conglomerates, 399; marine, 400, fluviatile, 401, glacial, 402, fanglomerates, 405; faulting in, 411; thickness of, 412. Mariposa Formation in the Vicinity of Colfax, California, The Brec- cias of the, 383. Mariposa-Calaveras unconformity, 406. Marquette district, Lake Superior, formation in, 8. Marsh, O. C., cited, 285. Martin, B., cited, 47, 49, 194, 225. Maryland, Miocene of, 226. Mascall formation, 427. Mastodontine types, 435. Matthew, W. D., cited, 129, 272, 277, 422, 435, 440, 537. Megalonychidae, 139, 151. Megalonyx, 258, 275, 283, 471, 473, 488, 491; compared with Nothro- therium, 140, 153, 159, 502-513; figure of phalanx of, 490. jeffersoni, 139, 143, 154. leidyi, 139. wheatleyi, 159. Megascopic features of breccia, 394. Megatherium, compared with Nothro- therium, 143, 145, with Mylodon harlani, 275, with Scelidotherium, 281. Mellor, E. T., cited, 403. Menominee district, Lake Superior, formations in, 8. Mephitis occidentalis, 470. Merced formation, fauna of, compared with related faunas, 48, 49, 227. Mercer’s Cave, Calaveras County, California, 467. Merriam, C. H., cited, 483. Merriam, J. C., 87, 111, 129, 255, 421 517, 523, 531, 535; erted, 40, 65, 139, 194, 217, 224, 226, 431, 463, 484. Merychippus, 78, 81, 122, 123. Merychyus, 441. Merycochoerus, 81, 441. Merycodus, 79, 81, 127, 431, 437; figures of, 126. Mesabi Range, geologic district in Great Lakes region, 6. Mesnard quartzite, 8. Mesaverde formation in Sunshine anticlines, Wyoming, 454, 458. Mexico, ore and garnet zones at Nelerdene 29, at Dolores Mine, Michigamme slate, 10. Microlitic facies, Leona rhyolite, 369. Microtus, 487. californicus, group, 487. Miller, L. H., cited, 464. Miller, W. G., and Knight, C. W., cited, 13, 14, 16. Minerals Associated with the Cry- stalline Limestone at Crestmore, Riverside County, California, 327; description of, 332. See also Chino Hill; Sky Blue Hill; In- trusive rocks. Minerals, sulphide, in Crestmore for- mation, 352. Miocene formation of Maryland, 226; deposits at Santa Cruz, 282, 284; faunas formerly described as, 421; ras of Idaho formation to, - Miocene Sediments near Tehachapi [546] Pass in the Southern Sierra Nevada, New Mammalian Faunas from, 75. Mixosaurus? natans, figures of an- terior limb, 67. nordenskioldi, 65; figure of anterior limb, 67. Moira, granite gneiss in southeastern Ontario, 11. Mojsisovies, E., cited, 64. Molthan, cited, 130. Mono, Pleistocene lake, 519. Monterey, phase of Miocene, 115. Monticellite, 342; analysis of, 3438. Moody, C. L., 39, 87, 388, 445. Moropus, 79. Morotherium, 285. Morrison formation, in anticlines of Sunshine, Wyoming, 450. Mowry shale, formation, 451; presence of fish scales, teeth, ete., 452; sig- nificance of, 458; descriptions of specimens from, 452; position in Sunshine anticline, 456. Murex (Ocinebra) concinna, 236. peritus, 47. tethrys, 236. Mya zone, 216. Index BS cer an Hawver Cave, 467, 470, 473, Teoee oF 66, 171; identity of foot material, 276: co-ossification of phalanges, 283. harlani, abnormality in skull, 140; structure of pes in, 267; tarsus, 269; astragalus, 268, 279, 282, 283; cuneiform, 270, 272, 279; meta- tarsus, 270, 272, 278; digits, 272, 278, 280, 285, composition of, 279; co-ossification, 275, 283; division of astragalar facet, 279; peculiar modifications in pes, 282: figures of: left pes, 269; middle cuneiform and metatarsal, 271; phalanges, 273, 275, 490; "tooth, 490; com- parisons, 270, 272, 275, 277, 278, 279, 281, 283, 284, 285, 286, of co-ossification 275. tenuiceps, 171; objection to, 172; figures of cranium, 176, 178. robustus, 167; characters of, 267, 268, 269, 270, 275, 277; figure of pes, 269; compared with M. har- lani in respect to phalanges, 275, 277, 283. Mylodont sloth, characters of, 166- 172; dentition of, 168; South er aa 169; Nebraska skull of, 72 Mylodont Sloths from Rancho La Brea, Further Observations on the Skull Structure of, 165; cranium, 166; mandible, 168; dentition, 168. Mylodontidae, 488; Scelidotherium, a member of, 282. Mylohyus in Conard fissure, 473. Mytilus kewi Nomland, plate showing, 315. Nacimiento River, California, Santa Margarita fauna collected from, . Louise, acknowledgment to, 139. Nathorst, A. G., cited, 64. Natica orbicularis, figure of, 47, 48, 63. Nebraska skull of ‘Mylodont sloth, Wz. Negaunee iron formation, 9. Nematherium, 282. Neohipparion, 431, 485, figures of, 119, 121, 123. gratum tehonense, 118. molle, 120; beds of, assigned to Santa Margarita formation, 297. Neotoma cinerea, 486. fuscipes, 486. Neotragocerus lindgreni, 526; figure of horncore of, 525. New Fossil Corals from the Pacific Coast, 185. New Mammalia from the Idaho For- mation, 523. 437, 441; [547] New Mammalian Faunas from Mio- cene Sediments near Tehachapi Pass in the Southern Sierra Nevada, 75. New Puma-like Cat from Rancho La Brea, 535. New Mustelid from the Thousand Creek Pliocene of Nevada, 21. Ber eri Triassic ichthyosaurians Newhill, ‘Golitients, 226, 228. Nomland, JeOe 185, 191, 46-50, 302. North American toads, 289. North Star Quarry, Sky Blue Hill, California, 329. North Yakima, Washington, 255. Nothrotherium, occurrence, 138, 164, 465, 467, 471, 488; comparisons, 140, 142, 148, 149, 163, 502, 513: review of species, 157-162; rela- tionships 162-163; co-ossification 275, 283; some conclusions, 163,164. graciliceps, 160. shastense, cranium, 139-148; figures of 1389, 141, 148, 147; figures of mandible, 149, 150; from Potter Creek Cave, 157, 158; from Rancho La Brea, 492. hawveri, 492; figures and measure- >ments of, 492, 493, 496-502, 504, 506-513. texanum, 160, 161. Nothrotherium from Rancho La Brea, Recent Studies on the Skull and Dentition of, 137; occurrence, nature, and distribution of mater- ial, 138; Brazilian species, 142; cranium 139- 148; mandible, 148- 151; dentition, 151-157. Oakland, California, conglomerate, of, 364. Occurrence of Ore on the Limestone Side of Garnet Zones, 25. Okenite, 351. Old World faunas, correlation of, with American Pliocene mammal faunas 442. Ogishke conglomerate, 7. Oldroyd, Mrs. Ida, acknowledgment to, 40. Omphalosaurus, 69. Ontarian division of geological time, 16, 17 Ontarian system, 16, series included in, 16. 293; cited, Ontario, Canada, southeastern, granites in, Opal, 352. Ore, on the Limestone Side of Garnet Zones, Occurrence of, 25; rela- tionship between ore and garnet zones, 26; examples of, 26-33; in- terpretation of, 35, conclusions, 37, Index Ore deposit, Leona Heights, California, 373; metallographic study of, 374; genesis of, 375; relation of fractur- ing to, 377. Ore deposits, relationship between ore and garnet zones, 25-37; examples: Washington Camp, Arizona, 26; Silverbell, Arizona, 27; Seven Devils, Idaho, 28; Velardena, Mexico, 29; Dolores Mine, Mexico, 31; Mackay, Idaho, 33; White- horse Copper Belt, Yukon, 33. Ore Deposits of the Leona Rhyolite, Geology and, 316. Oreamnos, 470. Oreolagus, 182. nevadensis, figure of teeth, 183. Orinda, Contra Costa Hills, Calif- ornia, faunal list from, 426. Osborn, H. F., cited, 437, 472. Ostrea titan corrugata, 306; plates of, 319, 321. Ovibos, 473. Owen, R., cited, 267, 272, 274, 279, 280, 283. Oxydation products in Crestmore for- mation, 353. Pacific Coast, New Fossil Corals from the, 185. Pacific Coast, Pliocene mammal faunas on, 424, 439; toads on, 289. Pacific Coast and Great Basin Pro- vinces of North America, Rela- tionships of Pliocene Mammalian faunas from, 421. Pack, R. W., cited, 112, 118, 120, 127, 193, 194, 195, 208, 224, 296, 297. Palaeolagus nevadensis, type species of Oreolagus, 182. Palms quartzite, 9. Pararctotherium, 108. Payette Eocene, relation of, to Idaho formation, 432. Pecten coalingensis, faunal zone, 216. crassicardo biformatis, 207; plate Ol o2a. deserti, 232: figure of, 243. egregius, 23; figure of, 243. etchegoini, 239; figures of, 245, 247. nutteri, figures of, 245, 247. wattsi; figures of, 245. healeyi, 47, 48, 49. hemphilli, 47. opuntia, 47. (Propeamusium) levis, 56; figures of, 63. proteus, 232; figures of, 243. terminus, figures of, 243. - wattsi var. etchegoini, 239. var. morani, 239. Pegmatite, 5, 329; composition of, 330. Percentage method of age determina- Loe limited degree of accuracy of, 25. Periploma clarki, 307; plate of, 325. Persia, Maragha fauna of, 442. Pes in Mylodon Harlani, Structure of the, 267; tarsus, 268; digits, 272; compared with pes of other mylodont genera, 278-284. Pessopteryx nisseri, 69. Pessosaurus polaris, figure of anterior limb of, 68. Phalarodon, 65. Phillips Ranch, California, fauna, 77. Phlogopite, 334. Picton granite, 11. Pilgrim, G. E., cited, 92, 107. Pinna bicuneata, 308; plate of, 317. Pinole Tuff-Orinda, fauna, 422; list of, 425; thickness of section, 424. Planops, premaxillaries of, 143. Planopsidae, 139. Platygonus (?), 471. Pleistocene Fauna of Hawver Cave, 461. Pliauchenia, 441. Pliocene, Etchegoin. See Etchegoin Pliocene of Middle California. Pliocene Bear, An American, 87; oc- currence, 88; dentition, 90; skeletal elements, 97; relationships, 105. Pliocene beds: of California, at San Pedro, 48, at Carrizo Creek, 185, near Sargent, 225; of Florida, 226; greatest thickness of, 193, 203, 227; stages of, 434; Idaho fauna included in, 434; correlation of deposits, 192; map showing local- ities of, 199. Pliocene Mammalian Faunas from the Pacific Coast and Great Basin Provinces of North America, Re- lationships of, 421; new faunas discovered since 1909, 422; outline map of occurrences of, 423; list of: Tulare, Etchegoin, and Pinole Tuff- Orinda, 425; Orinda, 426; Chanac, 426; sequence of, 427; Rattlesnake, 428; Thousand Creek, 429; Ric- ardo, 430; referred to Idaho, 432; sequence of, 434; Blanco, 434; Snake Creek, 435; Republican River, 488; sequence of, 438; Alachua, 439; time relationships, 439, 443; correlation with Old World faunas, 442. Pliohippus, 431, 435, 437, 528; from upper Etchegoin, 195. proversus zone, 117. Porphyry, quartz monzonite, 330. Port Kennedy, fauna of, compared with fauna of Hawver Cave, and of Conard fissure, 472. Post-granitic division of time, 12. Post-Keewatin time, two distinct per- iods of granitic invasion in, 10. Index Potter Creek Cave, California, Noth- rotherium from, 164; mammals from, 462; list of fauna from, 468. Pre-Cambrian Rocks of the Region of the Great Lakes, The Correla- tion of the, 1; classification of, 2, 3; eriteria of correlation, table 4, showing, 18. Pre-granitic division of time, 12. Prehnite, 351; analysis of brown var- lety of, 352. Prepotherium, 283. Preptoceras, absence of, in Hawver Cave, 470, 471. Presque Isle granite, 9. Proarctotherium, 108, 109. Proboscidean from Manix Lake, 518. Procamelus, 81, 441. Procyon psora, 470. Pronomotherium, 431. Prosthennops, 126. Proterozoic, confusion in use of term, 19. Psephis tantilla, 47. Pseudaelurus, 442. Pseudolestodon, 275, 277, 283. Purpura nanna, 310; plate showing, 325. turris, figure of, 253. Pyrite, 352; in Leona Heights, 367, 373, 374; figure showing gouge surrounding, 373. Pyroxene, 349. Quartz, 350. Quartz-monzonite porphyry, composi- tion and description of, 330. Quartzite, Mesnard, 8; Sturgeon, 8; Sunday, 8; Palms, 9; Ajibik, 9; Goodrich, 10. Quaternary system in Sunshine anti- clines, Wyoming, 455, 459; terrace gravels, 455; two periods of deposi- tion, 455; alluvium, 455. Radiolites, hamlini. referred to Cir- ripedia, 41. Rainy Lake, geologic district in Great Lakes region, 6. Rana draytonii, 289. Rancho La Brea, series of mylodont skulls from, 165; Mylodon har- lani found in, 268; amphibian remains in, 287; compared with Hawver Cave, 474; bison at, 519; fauna of, compared with that of Fossil Lake, and of Lake Lahon- tan, 518, 519, 520; wolf group from, 531; Felis daggetti found, 535. Rancho La Brea, An Extinct Toad from, 287. Rancho La Brea, Recent Studies on the Skull and Dentition of Nothro- therium from, 137. [549] Randville dolomite, 8. Ransome, F. L., cited, 208, 377, 398, 401. Rattlesnake formation, age of, 427, 492; list of fauna from, 428. Rautenberg, M., cited, 275, 277. Raymond, W. J., cited, 40. Recent fauna in the vicinity of Hawver Cave, 475. “Red rocks,” excluded in correlation of pre-Cambrian rocks, 5. Redtop Mountain, Wyoming, 446, 456. Reef (Serpula [?]), in Etchegoin, 216. Relationships of Pliocene Mammalian Faunas from the Pacific Coast and Great Basin Provinces of North America, 421; time relations, 439; correlation with Old World faunas, 442. Repossi, E., cited, 65. Republican River, Kansas, fauna from 437, 438, 440. Rhinocerotid, indet., 135; remains of, 1a Rhyolite, Leona, soil of, 362; physio- graphy of, 362; area occupied by, 362; extrusion as a lava flow, 365, 366; distribution, age of, 366; faulting, 366, rift valley, 366, presence of pyrite, 367; width, 367; thickness, 367; reducing effect of, 377; geologic map of, foll. 383. Petrographie characters, 368; four facies: felsite, 368, vitrophyric, 369, felsophyric, 369, microlitic, 369, distribution of, 370; minerals in, 371. Chemical characters, 371. Rhyolitie tuffs in Etchegoin, 208. Ricardo fauna, 116, 422, 430, 431. Ringold formation, Columbia River, Washington, 255, 256; plates show- ing, 267. Riversideite, a new mineral, 347; analysis of, 347; water determina- tion of, 347, 348. Rock Creek, Texas, Mylodon harlani from, 269. Rodentia from Hawver Cave, 486. Russell, I. C., cited, 256, 517, 518. Saddle Mountains, Washington, 263. Salinas Valley, California, 304. Samwel Cave, mammals from, 462; list of fauna, 469; fauna of later than that of Fossil Lake, 519. San Andreas fault compared with Haywards fault, 366. San Antonio formation, 364. San Diego, California, fauna forma- tion, 47, 49, 50. San Francisco Bay, conditions of depo- sition along eastern shore, 409-410. San Luis Quadrangle, Santa Mar- garita fauna collected in, 302. Index San Pablo, fauna of Mt. Diablo region, 115. San Pablo formation, 295. San Pedro Pliocene fauna, 48. Sandstone, in Mariposa formation, 391, figure of, 420; oil-bearing, in Grass Valley, Wyoming, 454. Santa Cruz ground sloths, 164, 282, 284, 286. Santa Margarita Beds in the North Coalinga Region of California, Fauna of the, 293; relation to other formations, 296; lithologic section of, 298, figures of 298; list of fauna of, 300; list of fauna of Santa Margarita northeast of Coalinga, 299. Santa Margarita formation, relation to Etchegoin, and other forma- tions, 200, 201, 228, 296, 297; once considered a division of the San Pablo, 294; described from San Luis Quadrangle, 294; palaeon- tology of, 295; terrestrial deposits above, 297; fauna of, in San Luis Quadrangle, 302, in the Tejon Hills, 302, from the type section, 303, from Nacimiento River, 304. Santa Margarita Upper Miocene, 115. Sargent, California, Pliocene beds near, 225, 227, 228. Sayles, R: W., cited, 404. Secapanus, possibly new species, 478. Scaphiopus h. hammondu, 289. Scapolite, 350. Scelidotherium, 275, 281; comparison of Mylodon harlani with, 280, 283, 284, 286. magnum, 280. Schansi fauna of China, 442. Scott, W. B., cited, 188, 152, 162, 282, 283 Seine series, Great Lakes Region, 7; area covered by, 7; cut by granite and granite greiss, 7; evidence of batholithic invasion, 7; rests upon complex, 7. Seine slate, 10. Sellards, E. H., cited, 422, 439, 532. Semele fausta, ‘ Door figure of, 249. Septifer margaritana, 308; plate show- ing, 325. Serpentine, 334, 387. Serpula (?) reef in Etchegoin, 216, 239, figure of, 239. Seven Devils, Idaho, contact deposits at, 28. Shaler, N.S., cited, 403. Shastasaurus osmonti, terior limb of, 68. Shoshone Mountains, rivers rising in, 448. Siamo slate, 9. 2 “a figure of an- [550] Sierra Nevada, date of uplift, 85; amphibolite belt of, 386. Silurian, use of term, 16. Silverbell, Arizona, ore deposits at, 27. Sinclair, W. J., cited, 138, 513. Siphonalia danvillensis, plate of, 327. gilberti, 51; figures of, 61. Skull and Dentition of Nothrotherium from Rancho La Brea, Recent Studies on the, 137. Skull Structure of Mylodont Sloths from Rancho La Brea, Further Observations on the, 165. Sky Blue Hill, California, 329-332, 334-353; plate showing, 354. Slate, Hanbury, Siamo, and Tyler, 9; Seine, and Knife, and Mich- igamme, in Mariposa formation, 389, 390; figures showing boulders in, 418, 420. Slover Mountain, near Colton, Califor- nia, remnant of limestone body, 329. Smilodon, 104, 480; in Hawver Cave, 467, 470; figure of, 481. californicus, 524. Smith, G. O., cited, 257. Smith, J. P., cited, 223, 399. Snake Creek, fauna, 422, 435, 437. Solen sicarius, 203. South American mylodont sloth, 169. Spade-foot toad, 289. Sphalerite, 353. Spherulites, plates showing, opp. 381. Spitzbergen, marine Triassic reptiles of, 53, 64. Stearns, R. E. C., cited, 41. Steeprock Lake, geologic district, Great Lakes region, 6; correlation of, 5. Stegodon, 435, 438. Stock, C., 87, 137, 165, 267, 461. Stoner, R. C., cited, 112, 125. Strata Referred to the Ellensburg Formation in the White Bluffs of the Columbia River, Age of, 255. Stream valleys, present, superimposed, upon pre-Recent, 363. Strongylocentrotus, 47. Structure of the Pes in Mylodon Harlani, 267; details of structure, 268; comparison with other my- lodont genera, 278, with Lestodon, 279, with Scelidotherium, 280; modification and specialization of, 282; relation of mylodont pes to supposed human footprints in Nevada, 284. Sturgeon quartzite, 8. Sudbury. See Temiskamian. Sulphide minerals, 352. Sulphide-rich solutions later than those forming lime-silicates, 36. Sulphides, genesis of, 36. Index Sunshine, Park County, Wyoming, Anticlines Near, 445; location, 445; physiography and drainage, 447; origin, 448; relation to older structures, 448; stratigraphy, 449; formations of, succession, age, and characteristics, 449; structure, 456, geologic history, 458; geologic map, foll. 459. Cretaceous system, 450-454; Ter- tiary system, 454; Quaternary system, 455. Sunshine anticline, 456; plate show- ing axis of, opp. 448; figure of section of, foll. 459. Gooseberry Creek anticline, position and structure, 457; plates showing, opp. 450, 454; figure of section of, foll. 459. Switzerland, Triassic ichthyosaurians in, 64. Sylvilagus auduboni, 488. Systematic Position of Several Amer- ican Tertiary Lagomorphs, 179. Systematic Position of the Wolves of the Canis Dirus Group, Note on the, 531. Taliaferro, N. L., and Moody, C. L., 445. Taxidea nevadensis, dentition of, 22. Tegula (Chlorostoma) pulcella, 235. thea, 310; plate showing, 327. varistriata, 311; plate showing, 327. Tehachapi Pass in the Southern Sierra Nevada, New Mammalian Faunas from Miocene Sediments near, 75. Tehuichila, Mexico, 107. Tejon Hills, California, Santa Mar- garita species collected in the, 302; thickness of accumulation in, 424. Tejon Hills, -California Mammalian Remains from the Chanac For- mation of the, 111. Teleoceras, 442. Teleopternus orientalis, 473. Temescal Lake, California, fault at, 367. Temiskamian series, in Cobalt, and Sudbury districts, Canada, 10; data of, 11; Hastings series cor- related with, 14. Temiskaming, Lake, sequence of pre- Cambrian rocks on, 10. Tephrocyon, 437. Terrace gravels in Sunshine anticlines, Wyoming, 455. Terrestrial deposits above the Santa Margarita formation, 297. Tertiary Lagomorphs (American) Systematic Position of Several, 179. Tertiary period, Wasatch formation deposited, 458. 21; figures of [551] Tertiary system in Sunshine anticlines, Wyoming, 454. Tetrabelodon?, 134; figures of, 134. Texas, Nothrotherium in Pleistocene deposits of, 138, 164. Thermopolis shales, near Sunshine, Wyoming, 450; conditions of de- position, 458. Third Street tunnel horizon, Los Angeles, California, probably Plio- cene, 41. Thousand Creek region, Nevada, ex- pedition to, 21; fauna of, 422, 428, 429; formation later than Virgin Valley Miocene, 429. Thracia formosa, 234; figure of 249. trapezoides, 47, 49. Thunder Bay, geologic district Great Lakes region, 6. Tillites, glacial, 402; Mariposa breccias resemble typical, 407. Titanite, 349. Toad from Rancho La Brea, An Ex- tinct, 287; lists of bones of, 289; sre divisions of, 289; spade-foot, 9. Tourmaline, 350. Tragocerus, 437, 442. Tremarctos ornatus, 93. Trematherium, discussion of deriva- tion of Nothrotherium from, 162. Triassic ichthyosaurs, 64, 71. See also Marine Triassic Reptile, fauna from Spitzbergen. Trophon belcheri avitum, 237; figure of, 253. perelegans, 311; plate showing, 327. raymondi, 53, figures of, 61. Tuff-Orinda fauna, Pinole, 422. Tuffs, Rhyolitic, in Etchegoin, 208. Tulare formation, California, relation of Etchegoin to, 202; period of deposition of strata below, 228. Tulare-Etchegoin section, thickness of, 424; list of fauna from, 425. Turris (Drillia) mercedensis, 47, 48, 49; figures of, 63. modestus, 54; figure of, 61. perversa, 47. Turritella cooperi, 47. freya, 312; plate showing, 325. jewetti, 47. margaritana, BY nova, zone, 216. Twain, Mark, 284, note 33. Tyler slates, 9. University of California, palaeontolog- ical collections in, 268. Umpleby, J. B., 25. Ungulata, from Hawver Cave, 513. Ursidae, 87. Ursus, compared with Indarctos? oregonensis, 102, 104. in 312; plate showing, Index Vaqueros, formation, 296. Vaughan, F. E., cited, 111. Vaughan, T. W., cited, 185. Velardena district, Mexico, 29. Vermilion Lake, geologic district in Great Lakes region, 6. Vitrophyric facies, Leona rhyolite, 369. Vesuvianite, 338; analysis of, 339; plate showing projection of cry- stals of, 360. Vulcan iron formation, 9. Waluewite, a variety of xanthophyllite, 341, 342. Wasatch formation in Sunshine anti- clines, Wyoming, 454; period of deposition, 458; figure showing, opp. 448. Wasatch glacier, evidence furnished by, on age of Fossil Lake fauna, 518. Washburne, C. W., cited, 447. Washington Camp, Arizona, ore de- posits at, 26. Watts, W. L., cited, 40. Weed, W. H., cited, 377. Whalen Creek, California, fauna from, 215. White, C. D., cited, 403. White Bluffs of the Columbia River, Age of Strata Referred to the Ellensburg Formation in the, 255; plate showing, 267. [552] Whitehorse oERes Belt, Yukon, ore bodies of, 33. Whitman, A. R., cited, 376. Wilkeite, 343; analysis of, 344. Willis, B., cited, 401. Wiman, C., 63. Winge, H., cited, 280. Wisconsin, or last glacial epoch, with reference to age of fauna of Lahontan and of Bonneville, 519. Wolves of the Canis Dirus Group, Note on the Systematic Position of the, 531. Wollastonite, types of, 334; analysis of, 335-338; plate showing pro- jections of, 358. Wolves of the Canis Dirus Group, Note on the Systematic Position of, 531. Wood River, Wyoming, 447; source of, 448; tributary of Greybull River, 448: relation to older structures, 448; history of, 449; plate showing terraces on, opp. 456. Woodruff, E. G., cited, 447. Wyoming, map of, 446. Wyman, L. E., acknowledgment, 166 176, 178. . . i ee r : = * : 7 . ca , ©. + ’ 7 ) : ‘ F 5 . ' ws ‘ ' ‘ 2 - 7 . . 4 . " . 1 me ~ , = : 7 i ‘ 5 a — ” L ate : ¥ 2 . é . ; 7 4 ¥ my 4 - ri ' . tT ‘i 4 Visit : aw ey ee ; i Tid opie Wy A ie can al a ae ‘] Tih, Rs ' i) Fa a ey hr ing RT eS YM Gada. on i en 9 SS" Oe «ef he | aimee bebo tht ba i 5 a.84 ; | Af *ryaper Aag , WANA Maaght ae ti en a Wy I] Mast ale iti} saa a sta” athlaaal s- > prpPha’ > ae ar? id tq ake apeibeaeteesen Ree tet gee td PS ont higan ropl hae @ a °F A as > « ite aacee toh & A aan jasnaete: alee LTE iligaaaa’ Yosng pnthsnnet? Q MRay ARAN, plat sueet! 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