Se a an re ee oe te Oa te Drake po te ) VOLUME 1. . The Geology of Carmelo Bay, by Andrew C. Lawson, with chemical analy- ses and codperation in the field, by juan de la C. Posada : Price, 25c . The Soda-Rhyolite North of Berkeley, by Charles Palache ; . Price, Ioc The Eruptive Rocks of Point Bonita, by F. Leslie Ransome ; Price, 4oc . The Post-Pliocene Diastrophism of the Coast of Southern California, by Andrew C. Lawson : f Price, 4oc The Lherzolite-Serpentine and Aneeed Rocks of the Potreo, San Francisco, by Charles Palache aves . On a Rock, from the Vicinity of Berkeley, ‘containing a New Soda Price, Ag Amphibole, by Charles Palache : 2a . The Geology of Angel Island, by F. Leslie Ransome, ‘with a Note on the Radiolarian Chert from Angel Island and from Buri-buri Ridge, San Mateo County, California, by George Jennings Hinde : . Price, 45¢ . The Geomorphogeny of the Coast of Northern California, by Andrew Cc. Lawson . Price, 30¢ . On Analcite Diabase from San Luis Obispo County, California, by Harold W. Fairbanks ; . Price, 25¢ . On Lawsonite, a New Rock- forming Mineral from the Tiburon Peninsula, Marin County, California, by F. Leslie Ransome . % Price, roc . Critical Periods in the History of the Earth, by Joseph Le Conte. Price, 20¢ . On Malignite, a Family of Basic, Plutonic, Orthoclase Rocks, Rich in Alka- lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, by Andrew C. Lawson : Price, 20c Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene, near Berkeley, by John C. Merriam. é Price, roc The Great Valley of Seg a Criticism of the Theory of Isostasy, by F. Leslie Ransome . ; Ps Price, 45¢ VOLUME. 2. . The Geology of Point Sal, By Harold W. Fairbanks . Price, 65¢ ..On Some Pliocene Ostracoda from near Berkeley, by Frederick Chap- man Price, Ice . Note on Two Tertiary Faunas from tie Rocks of the Southern Coast of. Vancouver Island, by J.C. Merriam . . Price, roc . The Distribution of the Neocene Sea-urchins of Middle ‘California, and Its Bearing on the Classification of the Neocene Formations, by John C. Merriam , r «> ~ Pricesioely: . The Geology of Point Reyes Peninsula, by FM. ‘Anderson : » Price, 25¢ . Some Aspects of Erosion in Relation to the Theory of the Peneplain, by W. S. Tangier Smith é Price, 20c . A Topographic Study of ‘the Islands of Southern California, by W. S. Tangier Smith “4 Price, 4oc . The Geology of the once Portion of the Isthmus of Panama, by Oscar H. Hershey ; . _ Price, 30c nea @antatacon to the Geology of the John Day Basin, by John C. Merriam Price, 450) ane . Mineralogical Notes, by Arthur S. Eakle “ .. . Price Toce aie . Contributions to the Mineralogy of California, by Walter C. Blasdale Price, 5c | The Berkeley Hills. A Detail of Coast a Peres Geology, by Andrew C. Law- son and Charles Palache P| : ‘ 5 o. Prices 80c UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 1, pp. 1=30, PI. 1. ANDREW C. LAWSON, Editor THE QUATERNARY OF SOUTHERN CALIFORNIA. BY Oscar H. HERSHEY. CONTENTS. PAGE HUfIaNt Te ATC UO Taree gerne scene ee Sa enna ee oca ac cae maa ate coe cee ee daveteenety Pentees ee 1 The Early Quaternary Orographie Disturbance ....... 02.00.00. eee 3 MMO M OLOT TAM VialLO YS) cree -c. etee. -geeccccesen pea nsectua Ste ceeedeceeses: The Santa Claran Epoch The Red Bluff Epoch and its Deposits The Later Quaternary Epochs........ 2.0.0.0... RSHEIGATOTE AY? 8 5 eB es OA Se Ee rea Pn os ; INTRODUCTION. Less attention has been given to the Quaternary geology of the State of California than the subject deserves. It has not proved attractive because of its simplicity. Impressive evidences of startling events, such as stimulate the student of glacial geology in the Hastern States, are here confined to isolated and often difficultly accessible localities. The Pleistocene fauna and flora were too nearly lke the present to be of great interest, until quite recently, to paleontologists in a land where there is such a wealth of older fossil remains. So it happens that, when all the fragments of knowledge which we possess in print of the Quaternary history of California are gathered together and sorted out, they do not even furnish us a satisfactory provis- ional scheme of classification to which to refer the various surficial deposits of the State. It is impracticable to apply here the scheme (with its various glacial and interglacial epochs) which has been evolved in the eastern portion of our continent. There is some analogy between bo University of California. [Vou. 3. our Quaternary events and those of the country east of the Rocky Mountains, but there is never any certainty that we are dealing with chronologic equivalents. In time, certain datum planes may be traced across the Cordilleran belt and our classi- fication tied to that of the Hastern States. In the meantime, only confusion could result from the use of the same epoch titles on the Pacific as on the Atlantic Coast. We have the same reasons for setting up an independent classification as exist in regard to Europe and the eastern portion of the United States. The above conviction will not prevent the writer from attempting to rationally refer, by means of erosion studies, the deposition of certain of our California deposits to about the same stages of the Quaternary era as certain drift sheets and associated phenomena in the Mississippi Basin. This is the special purpose of this paper, and Southern California is selected as the field of operation because in that section of the State the sequence of Quaternary events is most complete and the relative ages of the formations are most easily determined. Mr. Ralph Arnold has recently completed an extended study of the marine Pleistocene deposits of the Southern California coast. He presented a paper on the subject at the last meeting (December, 1901) of the Cordilleran Section of the Geological Society of America, but the full memoir is not yet in print. Through the courtesy of Mr. Arnold, I am in possession of his correlation table and can avail myself to a certain extent of the results of his work. I shall discuss this marine Pleistocene only so far as to fix upon its probable age as indicated by the erosion accomplished on it since its uplift. Aside from the marine terraces pretty thoroughly discussed by Lawson,* Fairbanks,T and Smith,} and the associated sands and gravels studied by Arnold, the Quaternary of Southern California is virtually a virgin field. *The Post-Pliocene Diastrophism of the Coast of Southern California, Bull. Dept. Geol., Univ. Calif., vol. 1, No. 4, 1893, pp. 115-160. t+ Oscillations of the Coast of California During the Pliocene and Pleistocene, American Geologist, vol. XX, October, 1897, pp. 213-245. tA Topographic Study of the Islands of Southern California, Bull. Dept. Geol., Univ. Calif., vol. 2, No. 7, September, 1900, pp. 179-230. BULL; DEPT. GEOL. UNIV. CAL. GEOLOGICAL RECONNAISSANCE SKETCH MAP OF SOUTHERN CALIFORNIA BY NS QS RESTLESS ROSS SOOSTS WN S LEGEND E3 Qneiss Petona Schists Archean Gneiss | San Eynedio Schists Ea Cambrian Series Granite Ravenna Plutonics | (Zi Cretaceous Saales EER San Pablo Series NS Rosamond series BMenenia Series ZEsconaiao Series ES Escondido Lava E25] Upper Phocene ees Tejon? Sandstone] Quaternary LOS AN ONTARIO Jcate ob/ Miles Hersuey.] Quaternary of Southern California. 3 THE EARLY QUATERNARY OROGRAPHIC DISTURBANCE. In the hydrographie basin of the Santa Clara River of the South, in Los Angeles and Ventura counties, there is an oval Upper Pliocene area about twenty miles long and ten miles in greatest width. After about 8,000 feet in thickness of gravel, sand, and elay (in part marine and in part alluvial, but all indisputably laid down in approximately a horizontally-bedded position and near sea-level) had accumulated, the basin was uplifted, compressed and the strata plicated. Around the border the gravel was tilted at angles prevailingly 20° to 30°, but near the center there was formed a distinct anticline, in the southwest limb of which the strata, even the very latest member, stand at angles varying from 30° to 60°, but prevailingly 45°. The orographie disturbance which thus tilted these late Pliocene beds was not an unimportant or local one.* Another and smaller isolated basin of Upper Phocene strata, lying mainly in the extreme northwestern corner of Los Angeles County, near Gorman’s Station, has been elevated bodily to an average altitude of 3,000 or 4,000 feet, tilted toward the center at angles of 10° to 30°, and profoundly eroded. On the eastern flank of Fraser Mountain, immediately northwest of this basin, there are several high mesas (altitude about 6,000 feet). They are remnants of old detrital slopes of light brown sub-angular eneissic debris, built up over tilted and eroded pink Upper Pliocene sandstone, and subsequently by uplift of Fraser Moun- tain, tilted more steeply away from the center of the mountain, raised high on its flank and deeply eroded. The detrital capping is late Quaternary. Fraser Mountain and the neighboring Sierra de la Liebre have beautiful dome shapes, and, as seen from a distance, smooth contours contrasting strongly with the rugged and no higher Alamo, San Emedio, Sierra Madre, part of the Tehachapi Range and the Coast Ranges in general in that region. These mountains and the similarly smooth ridge just north of Gorman’s * These beds are unconformably above a series of sandstones and conglomerates which are recognized as San Pablo in age, and on structural and lithologic grounds they are correlated with the Paso Robles formation, the Salinas Valley equivalent of the Merced series. 4 University of California. [Von. 3. Station were probably largely buried under detrital slopes and the Upper Phocene sandstones until the opening of the Quater- nary era. To explain the presence in late Phocene time of the sea in that basin some mountain has to be eliminated, and the evidence indicates the highest of the region, the Fraser-Pinos Range. Even if we will not agree that the Upper Plocene sandstone was at one time more extensive and covered the site of Fraser Mountain, a projection of the plane of the base of the sandstone series up the slope of the mountain will convince the student that in late Pliocene time the site of Fraser Mountain was a surface not appreciably elevated above sea-level. There is no faulting or any unusual type of deformation apparent. In (Quaternary time Fraser Mountain has been lifted to an altitude exceeding 8,000 feet, and most of this elevation was accom- plished during the disturbance immediately succeeding the Phocene period. The same argument applied to the Upper Pliocene basin in the Santa Clara Valley will lead to the same result. The high mountains almost enclosing the basin owe their present: prominence chiefly to uplift in early Quaternary time. This is especially true of the great mother range of Southern California, the Sierra Madre-San Bernardino Range, which has an average altitude exceeding 6,000 feet and several peaks reaching 10,000 and 11,000 feet. The only extensive portion of Southern California, so far as seen by the writer, apparently remaining nearly in its late Phocene condition is the Mohave Desert. Professor N.S. Shaler says* of it: “The most complete effacement of the original valleys appears to have taken place in the region known as the Mohave Desert. Here the detrital slopes have risen to near the tops of the ranges.” I entered the region with that idea in mind and came out convinced that it requires a radical modifi- cation. There are, indeed, thick accumulations of detrital material that have been built up close to the foot of such prominent ranges as the Tehachapi and the Sierra Madre, and may have buried the foot-hills, but in the central and by far the larger portion of the desert region I do not believe the detrital * Broad Valleys of the Cordilleras, Bull. Geol. Soc. Amer., Vol. 12, p. 290. Hrrsuny.] Quaternary of Southern California. 5 slopes have filled the broad basin-like valleys to a depth greater on the average than several hundred feet. Low knobs of granite occur at many places near the center of these basins, and where canons have been cut into the detrital material, as by Mohave River, hard rock has been encountered at many points at no great depth. There is an area thirty miles long by three to four miles wide, and another thirty miles lone by twelve to fifteen miles wide, of undulating granite comparatively free of detritus and characterized by long, broad, low, smoothridges in which the granite (much weathered and softened, ) is rarely more than ten feet beneath the surface, and is often uncovered by railway cuts at three to five feet. These ridges are surmounted by knolls of broken pegmatite, and in places rise into short, rugged hill ranges, but rarely reach the dignity of mountains. So strong was the impression that I was traveling over a country that had been reduced nearly to a uniform level by erosion, that it seemed natural to refer to it in my field notes as the granite platform. I should hardly lke to eall it a peneplain, as evidences of actual and completed base-leveling, if they ever existed, are now obscured by the more recent detrital slopes and alluvial deposits that floor the broad basins. It is a land whose topographic forms have reached the stage of old age but not that of senility. On the granite areas denudation effaced most of the rugged mountains and left only a few standing widely separated from each other. On a peneplain these would be classed as monadnocks. Where the rocks were more resistant, as on the gneiss, schist, quartzite, and limestone east of the main granite area, residuals were more numerous, and that region now has many rugged ranges. The relation between the granite and an overlying voleanic series, apparently of Eocene age, indicates that the surface of the former had been reduced nearly to its present level early in the Tertiary era, and the country was probably even more uniform in the Eocene period than at the present time. Many of the rougher ranges in the desert are composed of rhyolite resting on granite at a level not much above or below the general level of the basins. Faults of small throw are common, but do not appreciably affect the present topography. 6 University of California. [Vot. 3. Dr. H. W. Fairbanks thinks that we have in the Mohave Desert essentially the same topography as characterized the site of the Southern Sierra Nevada area before the great uplift to which the Sierran valleys are due; and also that the Sierra Madre- San Bernardino Range is a portion of this old lowland which was elevated by faulting at the close of the Pliocene period,* in which view I concur with some reservations. As Antelope Valley is a structural basin with a thick Tertiary and Quaternary filling, I am not quite certain that the high range on its southern border ras not outlined during a disturbance prior to that which opened the Quaternary era. Further, I suspect that some of its higher and more broken portions represent residuals on the late Pliocene plain such as are so common in the Mohave Desert, and with as much reason may have remained in force on the oro- graphie block which was subsequently thrust up into the present high range. However, I will agree that the attitude of the Upper Phocene strata bordering on it and the many deep, extremely narrow canons trenched into its mass, make it reason- ably certain that the range owes its present great prominence to uplift at the close of the Pliocene period. The Mohave Deserteand Antelope Valley were elevated as a whole, without any great deformation, something exceeding 2,000 feet. On the north, the Tehachapi Range was thrust up by the sharp tilting of a series of narrow fault blocks. At the same time the Sierra Nevada Range rose to its present prominence by the uplift of its eastern border to the extent probably of from 7,000 to 10,000 feet. The disturbance extended throughout the State. The Klamath Mountain region was deformed into great domes and arches, with elevation along the axes of several to the extent of 4,000 feet. The Coast Range region was uplifted and deformed from end to end. Among the best-known local evidences of this may be cited the faulting, tilting, and erosion of the Merced series on the San Francisco Peninsula and associated upthrust of Montara Moun- tain as described by Lawson,t and the upthrust of Mt. Diablo * Communicated. + Bull. Dept. Geol.. Univ. Calif., vol. 1, No. 4, pp. 148-151. Hersey. ] Quaternary of Southern California. 7 as determined by Turner.* It is evident that the territory of California at a time closely following on the deposition of the recognized Upper Pliocene marine deposits was the site of a profound orographie disturbance which radically modified its surface conditions. The wide extent and great importance of this disturbance have recently been recognized by other investigators.t It properly terminated the Pliocene history and inaugurated typical Quaternary conditions, so that it is perfectly natural to consider it the opening event of the Quaternary era in the State of California. I am informed that paleontologists (including Arnold) are finding a typical Pleistocene marine fauna in the upper portion of the Merced series and its Southern California equivalent, a series the greater portion of which is by common consent considered Upper Pliocene in age; and by them it is proposed to place the inferior boundary of the Quaternary era chrono- logically below the great orographie disturbance outlined above, a proposition to which I most vigorously demur. The line dividing the Pliocene and Pleistocene should be so drawn as to be of the greatest convenience to the greatest number of geologists. If the line is placed in the conformable strata below the physical break, it can only be recognized in a few limited basins, but if the great orographie disturbance which suspended deposition in those basins be accepted as the first Quaternary event, no difficulty will be experienced in properly placing it throughout the State. At most, there can be no great difference between a late Pliocene and an early Quaternary fauna. sy “se UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 2, pp. 31=50, Pls. 2=4. ANDREW C. LAWSON, Editor COLEMANITE SOUTHERN CALIFORNIA. A DESCRIPTION OF THE CRYSTALS AND OF THE METHOD OF MEASUREMENT WITH THE TWO-CIRCLE GONIOMETER. BY ARTHUR S. HAKLE. CONTENTS. PAGE IDEScmijouromnOnsCEYStals! rch csoeeecceece eneeceee coceien, ceeceetinects § 0+: ese 3) erat GUNG til Naeem arcane esc esc cc decgccasecteerese =e 1a. see PERN ee eset 352-2 OL FEN Gran 1 Lis mene eee cee see Set ern tos te s,s waster tieed de aisentiteeeeede HePessece Bo TR OVENS ee peers chs fe Aces erie reer 33 ING Was EOP Sei eeec se eres ches acct sedece ee cssts Fee ee I ae OY gan ios eeseanie cit KOO (ONG SSUES LEY 6) Ue ee ee it oe oe 2a ear ae 37 @ombpim ations) fee eeeeeeeee, toca ESET RE Ee os Ce ee 38 IerOveCHONS .. cet cece) eececesetertees A ee oy di, MERE I errors ... 39 Method............ Be Pee ie ne ede a Natta Seder see A Pe ra) PAC VINES CS een erect er Ee ee ee eee eee Bea ee re eee 40 Polar Orientation ......... a ae Ea PPE EY eM ol Shyiaall S/o) Op es eee ee ee Bee re: OS se ae Ne ce ee GTOMONICME TOF OCT OM ne aces cccd cee: sede ncceep seccaceaceec iecdessesrseceuesessecasigece Suesseie teed . 42 Determination of ¢, # and B Eee Rice) eee ete nee tare eter ees oe at Determination of p’, and q’ ........ ay p Reger eenapee reas eee ee GAD, Determination of the Polar Elements Po, Go AN € ........ 2. eee eee eee 44 Determination of the Axial Lengths @ and € oo... eee eee ence eee 44 ECORCMO maine mle ds URE MUOM Us eee cess. esse oe. senses cedesteasevietrey, csreseeceensesacssecetee= 45 Caleulated Table........2.... ee ees Dea ROR re So ee ee 48 DESCRIPTION OF CRYSTALS. Introduction.—The mineralogical collection of the Univer- sity of California includes several excellent specimens of colemanite, showing beautiful crystals in the druses and geodes of the massive material, and the abundance of good By University of California. [ Vou. 3. measurable crystals afforded an opportunity to make a very complete crystallographic study of this borate. The suite of erystals selected for measurement included probably all of the habits, and possibly all of the forms, possessed by the mineral. The measurements were made with the two-cirele (Zwei- kreisige) goniometer, designed by Goldschmidt. Since the method of measurement with this instrument and the gno- monic projection are as yet not generally understood by American readers, a detailed statement of the work follows the description of the crystals, which will make clear the steps used in the calculation and projection of the forms. Colemanite was first discovered in Death Valley, Inyo County, California, in 1882, and in the following year the more extensive deposits were found in the Calico District, about five miles from Daggett, San Bernardino County. Most of the fine geodal specimens are from the Calico District and it is presumed that the crystals described here are from this locality, as the labels indicate. The erystal forms of colemanite were first described by Jackson.* His description of the crystals was quite complete and forms the basis of what is at present known regarding their forms. Some of his crystals were from the Death Valley deposits, but the majority came from the Calico District. Others who have measured the crystals are: Hiortdahl,t who published a short description of the forms and _ optical properties, with a chemical analysis of a few crystals from Death Valley; Bodewig and vom Rath,} who likewise described some of the Death Valley crystals, and also gave an account of the origin of the deposits, and Arzruni,S who described one erystal. The crystals commonly line geodal-shaped cavities and some are quite large, one in the collection having a width of ten centimeters. They are colorless transparent, to white, although a few are stained yellowish by iron. Most of them *A,W. Jackson. Bull. of Cal. Acad. Sciences, 1885, No. 2, 2-36, and 1886, No. 4, 358-365. +Th. Hiortdahl. Zeitschrift fur Krystallographie, 1885. 10, 25-31. tC. Bodewig und G. vom Rath. Idem, 179-186. § A. Arzruni. Idem, 272-276. 9 Eaxue.] Oolemanite from Southern California. Sy) are attached to the matrix by one end of the vertical axis, leaving one end well terminated by front and rear forms. This circumstance rendered but one mounting on the gonio- meter usually necessary in order to measure all of the forms on a crystal, and measurements consequently could be rapidly made. Complete measurements were made of thirty erystals, and many more were examined for additional forms Hlements.—The axial ratio and angle 6 generally accepted for colemanite are those determined by Jackson. He derived his elements from the measurements of one crystal, but subse- quently verified his calculations by the examination of more erystals. By the two-cirele method of measurement all of the readings can enter into the computation of the axial lengths; consequently a ratio obtained by using a large number of readings from the best faces, is presumably more exact than when calculated from a few interfacial angles. As shown later in the detailed description of the work, the axial ratio and angle £, obtained for colemanite by the writer were as follows: a:b:c=0.7768:1:0.5430 ; B=110° 7 For comparison the elements calculated by others are as follows: Jackson, a:0:¢=0.7755:1:0.5415 : B=110°13% Hiortdahl, G06 —= O01 dat ts Ovotlio = 91 1013 Bodewig and vom Rath, a:b:¢ =0.7759:1:0.5416 ; 8 = 110°163” Forms.—The number of forms observed was forty-seven, of which thirteen were new. The forms are arranged in three columns below, those in the last column being new. The let- tering is the same as that given by Dana in his “System of Mineralogy.” Goldschmidt’s and Miller’s symbols are given for each form. The commonest forms are c, b, a, m, t, 4, «, h, B, y, v, d, and o. Less common, yet of quite frequent occurrence, are k, A, i, o, o, €, ¥, 2, U. The remainder of the known forms are rare: QY occurred four times, y three times, 7, h, V, twice, and e,q, B, ®, each once. W is common on one type of the crystals, but occurred only twice in the others. 34 University of California. [Vou. 3. ra Symbol. x Symbol. = | Symbol 3 | Gat. | Miter.) | 8 Bee oie. 3| Gat. | Miller. | ¢ 0 | 001 | Kia ot 311 7 30 | 310 1b!) Oo O10 | y} +10.1)10.1.1 p| +30 | 301 a 20 100 | é| +12 123 g | —207 79502 | ¢| 2c 210 | lke) 23? 83 f| —80 | 801 m Kn 110 | O13} 131 | +31 522 Z co 2, 120 | y —1 | Ill p | +325 e142 H 13 130 v —y 221 Dileep | él | «) O1 | OU q| —3 | 331 u| +43 | 164 | a 02) 1 2021 B= at eB) +3¢ | 165 A +20 201 ® —31 | 811 1/4 | +12 | 2382 Vv. +10 101 o0| —21 | 211 | P| 34. 3 i | —10 101 ¥| —32 | 2821 |) °* | 01) —=84) = ls2 || —20 | 201 € | 2p ue col s| —34 | 341 lw! —80 301 | CO) = 12 = y; —40 401 Q| —24 241 U| 60 601 Zi/e—13 131 B +1 111 r| —1$ | 232 The unit prism m is the predominating form, and the other prismatic forms are very narrow. Usually the rear face of @ is much broader than the front one; 0 is usually present as cleavage faces, and when the natural face does occur it is small. When the base ¢ and orthodome / are broad, the remainder of the terminal forms are small and usually few in number; on the other hand, when these two forms are absent, or very narrow, the other terminal forms are well-developed. As a rule the negative forms, that is, the upper rear forms, are larger and better developed than the positive ones. A steep pyramid occurs on a few of the crystals, but the faces gave very poor reflections. The best readings indicate the symbols }10.1.1} for the form, which are the same as determined by Jackson and cited as doubtful. Kieght forms given by Jackson were not observed by the writer. These are {370}, {10.19.0{, $19.19.6$, $7713, } 4125, {731}, {721}, and $711}. According to him, the faces of all these forms were extremely narrow, and gave either broad bands of light or no wedge-reflections whatever. In all probability {370} and {10.19.0} are 31203, and }19.19.6§ is {331}. Many of his original erystals were examined by the writer for these forms, but they could not be identified. Baxue.] Colemanite from Southern California. 35 New Forms.—With the exception of }341{, each of the new forms was observed but once. 7= 300}310{. This form was represented by a narrow face between $100} and }210¢. The reflection was bright and good. p p Measured 76°29" 90°0’ Calculated 76 20 90 0 p= +30)301{. This was a narrow bright face, but the image was only fair, and the p-angle varied somewhat from the caleulated one. > p Measured 90°2’ 69°33” Caleulated 90 0 68 57 g = —303502{. This form oecurred as a small triangular face, giving a good reflection. p p Measured 90°7’ 56°20’ Caleulated 90 0 56 12 f=—80}801}. This was a very narrow dome face, and the reflection was poor. The face occurred between }100{ and }201( in the same zone. ’ p Measured 89°23’ 80°13’ Caleulated 90 O 79 51 = +31}522(. This form occurred as a narrow face between 2311§ and 31115. It gave a fair reflection, but the angles vary somewhat from those calculated for the symbols. The symbols are the simplest and probably the most correct for the form. p p Measured 75°49’ 65°46’ Caleulated 76 18 66 26 p= +42$142}. This was a very small triangular face with a bright image. p p Measured 34°38" 52 Ag” Calculated Bue ue 52 43 36 University of California. | Vou. 3. u = +423164). This occurred on the same crystal as the pre- ceding, and was also small and bright. p p Measured 34°23” 44°98’ Caleulated 34 8 44 32 The next five of the following forms occurred on the same crystal. n—=+14}141(. Two faces of this form occurred. They were both well developed and gave good reflections. p p 979477 rs OPK o/s 27-11 67-5: Measured es 7 9 67 383 Caleulated 2D 67 42 m=+44 3165(. This was a very bright small face which gave a good reflection. p p Measured Be hie 39°40 Caleulated 38 19 39 43 n = +133232(. This was a narrow face with a bright reflection. Ge p Measured 58°41" 54°10’ Calculated 53. 44 54.1 P=— (1235. This form was represented by a small, well developed face which gave a bright image. p p Measured 18°307 male MO Calculated 18 5 20 51 s = —34}341}. Two large well developed faces of this form occurred on this erystal, and it was afterwards also observed on one other. The reflections were good. a p 1 { 40°50’ 70°50 Measured 40 48 70 46 BES MQ) BY) 70 52 Caleulated 40 40 70 45 Eakue.] Colemanite from Southern California. ot $45782t. The edge between }131{ and }110{ was replaced by a narrow face which was somewhat rounded, and did — not lie exactly in the same zone with these two forms. The symbols are the nearest simple ones to agree with the readings, although the measured and calculated angles do not closely agree. p p Measured 0.16 63°41’ Caleulated 0.09 64 16 Crystal Habit.—Four quite distinct habits are noticeable, and these will be designated as Habits 1, 2, 3, and 4. Habit 1.—Crystals of this habit are characterized by a broad base (001) and rear orthodome (201), the two faces meeting in a long edge, almost the width of the erystals. The prism (110) is long and almost meets the base, the unit pyramid (111) being merely a narrow truncating form. The pyramidal forms are small and grouped at the extreme right and left corners of the crystal. The clinodomes (011) and (021) are often absent. This habit exhibits the monoclinic symmetry of the crystals in a more pronounced way than the other habits do. This type of erystal is seen in Figure 1, Plate 2. The rear orthopinacoidal face (100) is generally broad like the dome (201). The clino- pinacoid oeeurs only as broad cleavage faces, and many of the erystals are cleaved into tabular plates parallel to this form. Habit 2.—In this habit the base and orthodomes are either very narrow or completely wanting. The clinodomes and rear pyramids are large and about equal in size. The crystals have a characteristic pointed appearance at the ends of the ortho- diagonals, the points being truncated by small natural faces of the clinopinacoid. Most of the crystals seem to be of this habit. Figure 2, Plate 2, shows this habit. Habit 3.—In this habit the front upper terminal faces are quite small, while the unit prism faces and the orthodome (201) are large. This gives a somewhat flattened appearance to the crystals, and at the same time causes them to be pointed at the ends of the vertical axis. This habit is quite striking, and the specimens are quite suggestive of dog-tooth spar. This type is seen in Figure 3, Plate 2. 38 University of California. [Von. 3. Habit 4.—The crystals of this habit consist essentially of the prism (110) and a broad steep orthodome (301). The com- bination of these two forms makes a very thin wedge-shaped crystal with sharp edges. Some of the other forms also occur, but they are quite subordinate to these, and do not cause a variation in the habit. The dome (801) has a rounded or wavy surface and seems to grade into a still steeper dome, probably (401) or (601). The form (301) is characteristic of this habit, and was only observed twice on crystals of the other habits. Figure 4, Plate 2, shows this habit with curved edges resembling spear heads. This habit was first described by H. S. Wash- ineton.* Combinations.—The erystals are so rich in forms that many of them have thirty or more faces. The various combinations observed were as follows: ee ) Cc, CG, a, t, m, K, 4, hy Ww, o, 8, 4, 0,0; ©, 0; Ff. t, m, 2, «, 4, 7, B, v, d, p, u. b, a, t, m, x, 4, h, 7, B, y, v, d, x, 0, €, w, Q. t, m, h, ¥, v, 0. Up HA alg Oo iy 104 Bin OA TER Oe , a, t,m, *,%, h, B, y, v, d, k,-o. a, t, mM, &, Ky %, Nh, Boa a. a,0, 01. a ? a, t, m, 2, K, 2, A, 4, B, y, v, ©, d, 0, g, Q. Ot, Hi, Ka, 0,10, 4 Uo. .€, b, a, t, m, «, 4,A,%7,h, 7, B, y, v, », d, C. b, a, t, m, 2, Ko, X, 4, h, o, B, vy, v, d,C, 0, OQ: a, m, 2, k, 0, 4, U, B, y, d,.a, €. b, a, t, m, *, 2,4, h, v, U, By o, y, v, 6,28. a,t, m,A,7, W, y, 9, d, Y, 5, p- a,t,m,V,h,¥, U, B, y, v, d, 0. Bb, @, 6, MK, @ 4, BY, v, 0, ds m, 2, H, «,«, B, d, x. OAs, 9, Ky Oe MeO a0) Ok Ets 2K, 0, By, We, Or mendes t,m, h, W, y, v, d. b. G, t, mM, @, Kk, a0, Bay ve @. de. *H.S. Washington. Amer. Journ. of Science (3), 1887, 34, 281-287 a Fake. ] Colemanite from Southern California. 39 22s -¢ a, t, m, 2, *, % h, U0, By, v, Od, @, 0,0; B, «. DG. Ode ie, HKG wN, 4. i ae, WO, O, a, bh, On P. 24. Ob 25. ©€ a,t,m.%, h, v, y, v, ad. b, a, t, m, *,%, h, ¥, U, B, y, v, a, o. DG Crbeils Ny Ky Cet WU, 8, .Y. UO.09 6d, €, Wika. 0, b.m,Koo, At, Wy, 8, 4,0, 0,2 Oy S,¥: Pe iG0. Gabi Kae no, Oo. B..%. 4, 7.0, 0. 29. c, b, t, m, 2, «, 4, B, y, v, a, d, ¢, Q. 30. c, b, a, m, «,%,7,h, ¥, y, v, g, d, o. Projections.—Figures 1-10, Plates 2 and 8, are chnographic ') g ’ ie projections to show the habits and some of the combinations. Figure 10 is a drawing of Crystal No. 5, which has the five new forms besides the two rare ones, e and y. The new form (341) is a large face on this erystal. About two-thirds of the erystal is broken, otherwise it would probably have shown a rich combination of forms, as most of the common terminal forms are missing’. Fieure 11, Plate 8, shows an orthographic projection on the ob rf * base of all the forms, with their relative predominance. Plate 4 exhibits a enomonie projection of the forms. The pole of the projection, represented by the dark circle, is almost midway between the projection of the base (001) and the dome ve the angles ¢ aud p for the faces (101), and since e’ is almost on the positive side of the pole vary only a few minutes from those at corresponding distances from the pole on its negative side. The erystals of colemanite therefore have an apparent orthorhombic symmetry, and the definite orientation of some of the crystals had to be determined by the direction of extinction on the clinopinacoidal section, this direction making an angle of about 6° with the vertical axis, in the acute angle Pf. The projection shows the excellent series of zones in which the forms lie. Most of the prominent zonal intersections on the negative side of the pole are occupied by faces, while on the positive side, several of these prominent intersections are not represented by forms, as, for instance, the cross zone 2po has only the one form (201) in it. Two of the negative pyramids, p(123) and w(182) have their projections on the positive side of 40 University of California. (Von. 3. the pole, and the latter form les almost on the first meridian. The pyramidal forms which are new are represented by two circles, and the direction of the prism (310) and dome (801) by double-headed arrows. In this projection the prismatic forms necessarily have no points of intersection, but their directions are shown by the arrows. METHOD. The two-cirele goniometer, with which the measurements were made, has been fully deseribed by Goldschmidt, together with detailed instruction in the calculation and gnomonic projection of the forms based on measurements with the imstru- ment,** and also in a briefer way by Palache.t Advantages.—This goniometer possesses manifest advantages over the ordinary reflection-goniometer, not alone in the sim- plieity and greater rapidity with which forms can be calculated from its measurements, but also because the two angular coérdi- nates definitely locate the form, and when these angles have been recorded for every known form on erystals, as Goldschmidt has done in his “Winkeltabellen,” a new form can readily be detected by comparing its angles with those recorded. It would be practically impossible to record all of the interfacial angles between known forms, consequently, as often happens, the measured interfacial angle is not given in the standard works on mineralogy, and quite frequently after long trigonometrical cal- culation the measured form turns out to be well known. The instrument, however, can also serve for the measurement of interfacial angles, and, in the opinion of the writer, is superior for this kind of measurement, as it really requires less time for the adjustment of the erystal. One adjustment of a crystal in true polar position is often sufficient for the measurement of all the forms, and in the case of colemanite, less than an hour was required to measure the most complex combination. *V. Goldschmidt.—Goniometer mit zwei Kreisen. Zeitschrift fur Krystallog- raphie 1893. 21, 210-232. Die zweikreisige Goniometer (Modell 1896) und seine Justirung. Idem 1898, 29, 333-345. +Charles Palache,—On Crystal Measurement by means of Angular Coordinates and on the Use of the Goniometer with two Circles... American Journal of Science, 1896 (4), 2, 298. BAKE, ] Colemanite from Southern California. 4] Polar Orientation.—Every face of a crystal has its position defined with reference to a pole and a direction assumed as first meridian, when its two angular distances, respectively, from these are known. By means of the graduated vertical and horizontal cireles of the instrument, these two angular cooérdi- nates, ¢ and p, are readily derived. The plane, normal to the prismatic zone is preferably chosen as the pole-face, and the ereat circle passing through the pole and the normal to the side pinacoid (010) as the first meridian. In systems with rectilinear axes the pole-face would then correspond to the basal-pinacoid, and the aneles for the three pinacoids would be $ p 001 0°00 0°00 010 0 00 90 00 100 90 00 90 00 Since monoclinie crystals have no plane normal to the pris- matic zone, the position of such a plane is best defined if prismatic faces are present. Colemanite possesses a well-devel- oped prismatic zone, including both pinacoids, so the polar orientation of the erystals was readily accomphshed. Each face of a erystal comes into reflection when it 1s normal to the line bisecting the angle between the telescope and collimator of the instrument, and this normal position must first be determined. Its angle on the horizontal circle H, is the ho reading for all measurements. The method of finding fo is quite simple. ‘Having the telescope tightly clamped at a convenient distance from the collimator, a bright reflecting surface is then mounted approximately parallel to the vertical circle, V, and centered. Tt is then brought at the intersection of the crosshairs by turning H and V, and the reading on H taken, = fy. V is then turned 180° and the reflection again brought into position by the adjustment tables and H. This reading on H = he. Then is ho = 3(A1—he). This ean be repeated until the reflection remains rigidly fixed at the intersection of the crosshairs, during’ a revolution of V. This final position of H is then the fo, and need never be changed. The crystal of colemanite was mounted with its prismatic zone approximately normal to V, and H was clamped at 42 University of California. | Vou. 3. 90° + ho. The reflection from the prismatic faces were, by means of the centering and adjusting tables, brought to revolve directly in the line of the vertical crosshair, on turning V, and the erystal thus brought into true polar position, because a plane normal to the prismatie zone would then be at ho. The reading on V for the clinopinacoid is the v» for this circle, which would be different for each crystal. Owing to imperfect centering or other causes, readings on V or on H for certain faces vary, when they should be the same; consequently both vo and fi. can be corrected by averaging the different readings. When the reflection of each face is brought at the intersec- tion of the crosshairs, two readings, one on V = v, and one on H=h, ave made; the face is then defined by two angular coordinates, ¢ = v—v. and p = h— ho. Symbols p q.—In place of the three indices of Miller for a terminal form, Goldschmidt uses the two indices p and q, and for calculations, and in the gnomonie projection, the two indices are preferable. The indices of Miller are readily transposed into those of Goldschmidt by making the last one equal to unity and not expressing it; thus 522 (Miller) becomes 31 (Gdt). Fur: thermore 001 = 0, 100 = »0, 010 = 0m, 110 = mw, 210 = 20 = : *,120 = x. When p and ¢ are equal, but one is expressed, thus 331 — 3. The zonal relations of forms are better shown by the two symbols, because all forms having the same p, or the same q, lie in the same straight line or zone; for example, it can be seen that the forms 73, $3, 53 are tautozonal, whereas their Miller equivalents (564), (296), (8.15.10) do not show this relation so well. Gnomonic Projection.—This projection shows the points of intersection of the face-normals, drawn from the center of the erystal, upon a plane lying preferably normal to the prismatic zone and at a unit’s distance from the center of the erystal. If h is the distance of this plane above the center and is equal to the c-axis, and 7, is the length of the base normal, then in erys- tals with rectilinear axes 7o = h—1. In monoclinic crystals the base is oblique to the plane of projection, and with h = 1, 1 1 ; 5 ro ig equal to Ga B = Tain jee whenee it follows that with 7,o=1, then h = sin p. EAKuE.] Colemanite from Southern California. 43 If with aradius of h = 1 = c-axis, a circle is deseribed, then this circle would represent in ground plan a sphere of projection. The plane of projection would be tangent to this sphere at the end of the c-axis, S would be the pole of the projection, and SY the first meridian. Any face pg would have the poimt of imter- section of its normal with this plane, located by the angle ¢ which it makes with the first meridian SY, and the distance from the pole d= te p. (Figure 1). The face py is further defined by the two rectangular coérdinates 2 y’, whose values deduced from the right triangles are « = sin ¢ tg p y = cos ¢ te p. By means of the measured angles ¢ and p, all forms can be plotted on cross section paper, and the co- . td Y . ordinates v y give graph- ically the symbols for any > Ll a f / form in terms of the x y of the unit form pq. In Fig. 1. monoclinic crystals — the projection of the base-normal lies in front of the pole at a dis- tance e’ = tg p, and the distances po and qo ave the cobrdinates for the unit pyramid pq reckoned from the base; therefore for any values of pq, « = pp’o te’ and y’ = qo. Determination of e’, », and B.—An average of twenty read- ings on the basal pinacoid gave p = 20°7, with ¢ = 90°; e = te p = 0.3663. This value of e’ was also obtained from the readings of the clinodomes. For these forms 2’ =e’, and an average of forty-four values of 2 for the domes 01 and 02 gave x = 0.3663: thus agreeing with the direct measurements. Also @ = cot » = 69°53’ and 6 = 180° —» = 110° T. Determination of p’o and q/o.—By means of the two formulae x =sin ¢tgp y = cos ¢ te p the codrdinates 2 y’ were calculated for all the best faces. For 44 University of California. [Vor. 3. the positive forms pp’o = # —e’, and for the negative pp’o = x +e. The symbols pg are simple multiples of the codrdinates, Pogo of the unit form, therefore the values p’oq‘o are readily deduced for each form. Taking fifteen of the best erystals as sufficient for the caleulation of the elements, the averages of p’o and q’o were as follows: Oo 0.74311 12 meas. Oo = 0.5438 12 meas. 7431 Oe 5426 Ones 7441 oe: 5435 9.23 7425 (a 5426 Ti ah 7447 i 5426 iw 7452 iy = 5435 ie 7452 1 ee 5432 114 a 7444 Bite 5429 8: ite 7449 ioe 5417 Oey am 7435 1B 5424 oe 7450 too 5436 16 7447 135 Ss 5423 i Saeae 7453 6. = 5437 6 bn 7446 8 * 5425 shies 7448 16.9 5431 L650 an Average 0.7443 = 165 0.5430 “11655299 The elements for colemanite are therefore po 0.7448 ; g’o= 0.5430 ; & = 0.3663 ; # 169536 The values 1 po, go, and e’o are the elements when h = 1 and ro = sn therefore when ro = 1, these values must be multiphed by sin p, Determination of the Polar Elements po, qo, and e. . / . to obtain the polar elements po, go, ande. Thus po = p’o sin p, . / . qo = gosin B, and e = eosin # = cosp#. The elements for colemanite then become po = 0.6989 ; go = 0.5098 ; e = 0.8439. Determination of the Axial Lengths a and c.—In systems with rectilinear axes g’o = tg(001:011) and p’o= tg(001:101); there- fore with axis 6 —1, the formulae for such systems become ¢ Lo y y (0 and &@& =-;, = lime i? d Po Po BaKue.] Colemanite from Southern California. 45 . . . or . / In monoclinic crystals, ¢ is also equal to the codrdinate ¢ 0; : er : a : ; the clino-axis @, however, is equal to nat therefore the form- b , wee ¢ 7 / 7, ulae for monoclinic erystals, in terms of pogo or pogo, when b = 1, become ; ; Lo s do YL ¢ do i — cE a, Le —_ = ito : sin po Sin ph Po Po Sin p, From these equations, @ = 0.7768 and ¢ = 0.5430; giving the axial ratio for colemanite @ : b : ¢ = 0.7768 : 1: 0.5480. Record of the measurements.—As an illustration of the actual measurements and method of deriving the symbols for the forms, the work on Crystal 23 is given. Each crystal was sketched before measuring in order to show the relative size of the faces, and the faces were provisionally lettered. The kind of reflection was designated as good, fair, or poor (g. f. p.). Starting with the angle on the side pinacoid (010) = 139° 44’, and plotting the v-angles in a cirele in the direction of the hands of a watch, it is easily determined which forms are positive and which negative. The h, for the instrument was 57° 54’, and the vo for the erystal was 139° 44. From the columns pp’, and qq’, the symbols pq are at once apparent, since po = 0.7443 and q’, = 0.5480. The record is simply a sample page of the note book, and it illustrates the simplicity and shortness of the work required to determine any form, as well as the neatness and compactness of the whole method. Reflections. 46 University of California. [Vou. 3. | Prisms = tg fo) pp'o fi | = Sal eas Sym rn ce) | ap = ; x e £ v h | Ig sinh lg a’ | x’ (positive) 440 bols pa v— Vo | h—ho lg tan p Aa | / =g/+¢/ ae lg cos @ oo | of (negative) | eee ees | | | 7 | b 139°44 147°54 0°00 90°00 9 | 0 m 193 40147 54|53 56/90 00 1.3730 x t 209 27147 54) 69 43 90 00 2.7058 2 & a 229 44147 54 90 00 90 00 9 ow 0 t’ 249 46147 54 69 58 90 00 | 2.7400 | 2 w | ~/ | m’ 265 44147 54 54 00 90 00 | eS) | go b’ 319 44.147 54 0 00 90 00 0 (i) es t” |354 20147 54 34 36/90 00 0 Bele oo 2 1 1345 07147 54/25 23/90 00 0.439 oo 3 m. 13 43.147 54/53 59/90 00} | 1.3752 wn | © sel o.cgasee| 1.8559 |1.4896/ 0 [+20 xv 229 43.119 35) 89 59 61 41) 0.268556 0.268556 | *-999 | : ie | ce) oa 0 | | sil at, stim SE SM ee Re ‘ i ; ce |229 43) 78 01] 89 59/20 07 =} Q031T oe 0 9.953537 | 9 pani ee p 203 42108 54 63 58 51 00 0.091631 seacounl hei 0.7433 0.5420 +11 9.642360 “""" Wee 3 POO0GO TA wy renee leet Plaees En PSR 2 "| 0.413356 | 2.5903 g |217 55/127 12] 78 11] 69.18) 0.429659 | O’sasace | 2475 | 2-2240 | 0.5419 |+3 1 : O | pili 0.5416 pines eu eae | wee | | | | | 9.990777 Saal eden g’ 241 30127 15 78 14) 69 21) 0.423807 Neacceal 2 D077 | 2.9814 | 0.5411 |+31 9.309474 | “7'°°* et GVOSBDSDIIY, aatena | ces h 243 55123 40\75 49/65 46! 0.346674 | Weseeeal ee 1.7876 | 0.5443 |+3 1 OSS9O Ty Sane eee an | OV ODTBGT | aeiaarenleodeae ad i \261 51/129 39/87 58/71 45] 0.481814 | P-ooocen | aaron | 22022 | 1.6123 [+33 QeT 5 GO2 (isa eee Mee mana 9.953599 | 9 ayanns | f p’ |255 45/108 57| 63 59/51 03| 0.092406 | O'osccye | g:sany | 0-7454 | 0.5427 |-F11 ORG 42101) |e omnes iar sali 9.505934 |.

Pay F g.| k | 23 58|109 14/64 14/51 20/ 0.096803 | O-rashc0 | o'5493 | 14917 | 0.5483 21 | | 9.638197 | ~” | 958569341. 4 nernee ae | | -_ 0.051075 1.124 SON wa g.| | 5 44/115 18/46 00'57 24] 0.194141] Opasmio| roses | 1-4910| 1.0862 |—22 | | | 9.841771 | feo | | | Ro rindoiGilln pantie! 4 amon Place g.| k’ | 75 30109 11/64 14 51 17/ 0.096027 | Meee a 1.4897 | 0.5423 —21 | 9.638197 48 University of California. [Von. 3. Calculated Table.—Following is a calculation of the 47 forms to correspond to the tables arranged by Goldschmidt in his “Krystallographische Winkeltabellen.” colemanite given by the writer are based on the elements po = The ealeulations of 0.6989 ; go= 0.5098, and e = 0.3439, and therefore show a slight difference in the angles from those given by him on page 100. a= 7768 ce = 5430 \ B if 69° 53” lg h lg sin po J lg a = 9.890309 | Ig ¢ = 9.734800 lg po = 9.844415 | do = 1.4306 | po = 6989 | lg do = 0.155509 | | lg bo = 0.265200 lg do = 9.707463 | bo = 1.8416 | Go = 5098 Gat. Miller. 001 010 100 310 210 110 120 130 O11 021 101 201 301 101 201 502 B01 401 601 801 Aya Jub Til pal 331 141 131 loor6es | 1° Lo sseaza 1g 22 = 0.136952 | h = 0.9390 | -e = 3439 | Ig cos p J do | | a! , | p p £o No | é n | (Prisms) y’ oe | | (a:y) SIP (90°00 20°07 (20°07 | 0°00 | 20°07 | 0°00 | 0.3663 0 | 0.3663 0 00 90.00 0 00,9000, 000 9000 0 Pa wo 90 00 90 00/90 00, 0:00 90 00, 000, % 0 os 76 20| ‘190 00|76 20 |13 40] 4.1227 | ow | « 69 58| * «| «© leg 58/20 02) 2.7419 |“ 5 53 53'| * a «¢ 153 53°|36 067| 1.3709 |“ at 3496] * eo | (134 96 (55 34| 006854 |“ se 94 33] «* «| lea 337165 26+) 0.4570 |)“ ms 34 00 |33 13°20 07 |28 30/17 50°|27 01 | 0.3663 | 0.5430] 0.6550 18 38/48 54| ‘* /47 22/13 56/45 34/ “* | 1.0860/1.1461 90 00/47 59/48 00| 0 00/4759! 0 00/ 1.1106 | 0 {1.1106 ‘* 161 40/61 40] ‘‘ |61 40} ‘“* | 1.8549) ‘* {1.8549 ‘¢ 168 57168 57°) ** |68 57-| ** | 2/5999)1| seem ingue 90 00 |20 42°)20 427) ‘ |20 42) ‘* | 0.8781 |) ‘ 0.8781 ‘ /4g1g|/48 18} “© |418!| “. | T1923 | “ |1.1998 “* 156 18|5613| ‘* |5613| ‘* | 1.4944] ‘ |1.4944 ‘“ 161 49/61 49; ‘* |6149| ‘‘ |T.se6e |] ‘* |1.8666 * 169 02 (69 O27 ae ViGON02) | ae 2.6109 | / “* | 2.61109 ‘176 17:17617| ‘* |7617| ** | 40996 | ‘* |4.0996 ' leg 51179 51| “* (75 51] ** | 5.5882) “* ipsgse 57 55 |71 56/68 57 58 27°53 40 30 19°| 2.5992 |1.6290|3.0675 63 56151 02/48 00 |28 30/44 18/19 58 | 1.1106 |0.5430/1.2362 34 51/33 29:20 42) ‘f |18 23 |26 55°} 0.3781 + 0266) 7 56/57 22 FB 18 47 22 37 14° 35 51 | 1.1223 | 1.0860/1.5617 48 53 68 01 GI 49 58 27° FF 19 37 34 1.8666 | 1.6290 2.4776 27 05 |67 42 |48 00 |65 17 |24 54°155 28 | 1.1106 | 2.1720] 2.4396 34 17/63 06'| ‘* |58 277/30 09/47 28| ‘* |1.6290|1.9716 os | | EAKLE.] a = 7768 lg a c = 5430 | ge = \lgk= —£ j ave ve | 2 a = ——S No z | Gat. | Miller. 4 | 28 | ly 121 29 | » |+13 | 232 30 | r |—13 | 339 81 | d|—12 | 121 32 | « —13 131 B30) CO l-- 10:1! 10.1.1 34 | & I+81 311 35 | @|+51 | 522 36, 0 —21 21] 37) ®@ 31 31] 38 BB o—41 411 SORtemi— 23: 23 40 Q 24 241 41 |) s |\—34 341 42 y —32 Bpal 43 | w |—i4 182 44 | p |+42 | 142 45 | w |+¢3 | 164 46 |p i|+3¢ | 165 47 P\|—i2 | 123 University Colemanite from Southern California. lg Po 49 9.890309 | lg do = 0.155509 9.844415 ee . 1.4306 Do 6989 9.734800 | lg bo = 0.265200 lg do 9.707463 bo 1.8416. do 5098 yp) 2972068 | i. aa | 9.536474 lee = 0.136952 hk = 0.9390" ¢ = 3489 re | Pa | co) | p &o | No Fa ny \(Prisms)) y! | os | (a: y) | tgp |45°38 prs: 48°00 47°22 36°57 36°00" 1.1106 1.0860 1.5533 [53 44154 01 ie 39 10 140 44 |98 35° a 0.8145] 1.3772 24 54/41 55°120 42] ‘* {16 20/37 18] 0.3781 |1.1100/ 0.8980 JTS 11/48 59°] ‘* |47 22/14 22 \45 a7] /1.0860 1.1500 13 04/59 07] ‘‘ |58 27°)II 11 |56 43° oe 1.6290 1.6724 86 017/82 43 |82 42°28 30 81 42° 3.57 7.8093 0.5430 7.8281 78 12/69 22/68 57) ** |66 21/11 02/2.5992 | ** |9.6553 76 18/66 2¢/65 49| ‘© |62 56/12 32°] 2.2270] ‘* {2.2999 64 11/51 16/48 18| ‘* |44 36°/19 52 | 1.1223 ‘* 11,2468 73 47 |62 47/61 49| ‘* |58 38/14 23/T.see6 | “* |1.9441 78 15/69 26:|69 02} ‘* |66 27/10 59, 2.6109 ‘| 2.6663 |/B4 34/63 11/48 18 |57 27°|30 25 47 18| T.1223 1.6290) 1.9782 37 19'167 45] ‘* 165 17 |35 08155 19 *¢ 19.1720) 2.4450 40 40°')70 45 |61 49| ‘* |37 58°/45 43°| 1.8666 ‘* | 2.8640 59 48/65 09| ‘* |47 22151 39:\27 09} ‘* |1.0860/2.1598 0 09°/65 17] 0 20/65 17 0 08°65 17] 0.0058 2.1720' 2.1715 |34 12°/52 43 [36 26°/47 22 26 34 41 08" 0.7384 |1.0860 1.3133 34 08 44 327/28 55/39 10 |23 11 |35 29°! 0.5523 |0.8145) 0.9841 38 19/39 43 |27 15 ee 05 23 20°30 05 0.5151 0.6516 0.8306 [18 05 |20 51] 6 44/19 54) 6 20°19 46° 0.1182 0.3620 0.3808 of California, April, 1902. VO Saar ens: BULL, DEPT. GEOL, UNIV. CAL. Colemanite. Ss WO OY GY. v VAX VADER VALERY = x State UNIVERSITY OF CALIFORNIA PUBLICATIONS verre ‘y Bulletin of the Department of Geology Vol. 3, No. 3, pp. 51-62. ; ANDREW C. LAWSON, Editor ‘ e THE EPARCH4ZAN INTERVAL an) * ass Cat A criticism of the use of the term Algonkian : a i Gon BY Yat x - y ease. e ANDREW C. LAWSON esonesneean, % fo, Ye CEE Ss S QW SS *E Hi Ee MV £27 Se es 12), 27S wee 7 \\ = S&S = if \ OF — fey G TSS) Ad hts : i DAT ZED om a3 BERKELEY a Sic THE UNIVERSITY PRESS a Cade 1p Soe ! MAY, 1902 PRICE 10 CENTS THE BULLETIN OF THE DEPARTMENT OF GroLocy OF THE UNIVERSITY OF Cant FORNIA is issued at irregular intervals in the form of separate papers or memoirs, en embodying the results of research by some competent -investigator in geological science. It is designed to have these made up into volumes of from 400 to 500 pages. The price per volume is placed at $3.50, including postage. The papers composing the volumes will be sent to subscribers in separate covers as soon as issued. The separate numbers — may be purchased at the following prices from the University Librarian, J. C. Rowell, to whom remittances should be addressed:— VOLUME 1. No. 1. The Geology of Carmelo Bay, by Andrew C. Lawson, with chemical analy- ses and codperation in the field, by juan de la C. Posada : Price, 25¢ No. 2. The Soda-Rhyolite North of Berkeley, by Charles Palache : 2 BICee OS No. 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome ; Price, 40c No. 4. The Post-Pliocene Diastrophism of the Coast of Southern California, by Andrew C. Lawson é f Price, 4oc No. 5. The Lherzolite-Serpentine and Associated Rocks of the Potreo, Sal Vie are Francisco, by Charles Palache woe No. 6. Ona Rock, from the Vicinity of Berkeley, ‘containing a New Soda Price, 300 | Amphibole, by Charles Palache No. 7. The Geology of Angel Island, by F. Leslie Ransome, ‘with a Note on the Radiolarian Chert from Angel Island and from Buri-buri Ridge, San Mateo County, California, by George Jennings Hinde . — Price, 45c No. 8. The Geomorphogeny of the Coast of Northern California, by Andrew C. Lawson 0 - Price, 30c — No. 9g. On Analcite Diabase from San Luis Obispo County, California, by Harold W. Fairbanks 4 Sy Pree 2 5c No. io. On Lawsonite, a New Rock- forming Mineral from the Tiburon Peninsula, Marin County, California, by F. Leslie Ransome . 5 Price, oc No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte. Price, 20¢ No. 12. On Malignite, a Family of Basic, Plutonic, Orthoclase Rocks, Rich in Alka- lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, by Andrew C. Lawson : ' Price, 20c No. 13. Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene, near — Berkeley, by John C. Merriam. ; Price, LOGS No. 14. The Great Valley of Coteus) a Criticism of the Theory of Isostasy, by ‘ F. Leslie Ransome . é % Price, 45c VOLUME 2 No. 1. The Geology of Point Sal, By Harold W. Fairbanks " Ve RTI CeAOSe No. 2. On Some “Pliocene Ostracoda from near Berkeley, by Frederick Chap- pee man . Price, Teena No. 3. Note on Two Tertiary Faunas from the Rocks of the Southern Coast of. Vancouver Island, by J.C. Merriam . 2 Rricky aioe No. 4. The Distribution of the Neocene Sea-urchins of Middle “California, and Its Bearing on the Classification of the Neocene Formations, by John C.© y Merriam i P ‘ Price, roc h No. 5. The Geology of Point. Reyes Peninsula, by F M. Anderson. - JPricey25e No. 6. Some Aspects of Erosion in Relation to the Theory of the Peneplain, by W.> é S. Tangier Smith ; Price, 20c © No. 7. A Topographic Study of ‘the Islands of Southern California, by °W: S. Tangier Smith é Price, 4oc No. 8. The Geology of the Central Portion of the Isthmus of Panama, by Oscar H. Hershey : : Price, 30c No. 9. A Gontibation to the Geology of the John Day Basin, by John C. Merriam : Price, 35c No. 10. Mineralogical Notes, by Arthur S. Eakle , Price, IOC «= No. 11. Contributions to the Mineralogy of California, by Walter C. Blasdale Price aie No. 12. The Berkeley Hills. A Detail of Coast st Range Geolesy by Andrew C. Law- — sou and Charles Palache . : 0 a 2 SPECES pes . UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 3, pp. 51-62. ANDREW C. LAWSON, Editor THE EPARCHAAN INTERVAL A CRITICISM OF THE USE OF THE TERM ALGONKIAN BY ANDREW C. LAWSON In the year 1854 Logan proposed the name Laurentian for a series of rocks, which he and his assistants on the Geological Survey of Canada had been studying for the preceding nine years in the region of the St. Lawrence and Ottawa rivers. He had in earlier reports referred to the same rocks as the “meta- morphie series,” and had shown conclusively that a part of them at least, comprising limestones, quartzites and conglomerates, were clastic rocks. In subsequent reports, and especially in the summary report of 1863, the term became very much extended, and vast terranes of granite-gneisses, anorthosites, ete., were included under it, as well as more evenly banded or bedded gneisses. By reason of their association with the recognizably clastic rocks, these granite-gneisses, anorthosites and banded eneisses were regarded as also of metamorphie derivation from original clastic sediments, and various attempts were made to treat them stratigraphically. With the progress of exploration it became apparent that this vast complex was resolvable into three subdivisions, and these became known as the Lower, Middle and Upper Laurentian, the first consisting of granite- eneiss, the second of lmestones, quartzites, conglomerates and banded gneiss, and the third of anorthosites. These subdivisions 52 University of California. [Vou. 3. were also known as the Fundamental gneiss, the Grenville series and the Norian series, respectively. To-day, no one qualified to speak upon the question enter- tains the idea that the Fundamental gneiss or the anorthosites of the Norian series are other than true igneous rocks. The Gren- ville series, however, remains as Logan interpreted it, a strati- eraphie sequence of clearly recognizable clastic rocks, with perhaps certain admixtures of igneous material: The term Huronian was first used by Logan and Hunt * in 1855 for the rocks of the north shore of Lake Huron and their supposed equivalents on Lake Superior, now known as the Keweenawan series. The rocks were at this time thought to be probably of Cambrian age. In the work of the next few years, the Upper Copper-bearing rocks of Lake Superior were segre- gated from those on Lake Huron and the term Huronian retained for the latter. In the report of 1863 the Huronian was described and mapped as a clastic series of pre-Potsdam age, with certain voleanie admixtures. Although it is probable, as I first sug- gested,? that the Huronian as deseribed in the report of 1863 embraces more than one series of rocks, yet no one has ever called in question the essentially clastic character of the great bulk of the rocks so designated. Both of these terms, Laurentian and Huronian, signalized most important discoveries in geological science. They were immediately adopted and widely used both on this continent and in Europe. The rocks comprised in these two series were re- garded as of exceptional interest because they antedated the Paleozoic and were separated from it by a profound and. wide- spread unconformity. This gave them a certain individuality as a whole which it seemed desirable to recognize by the use of a comprensive designation. Moreover, there might be other pre-Cambrian series of clastic rocks resembling the Laurentian or Huronian, the correlation of which with either of these series might be very doubtful, and the‘progress of the science demanded a comprehensive term which would not necessitate correlation of its members in widely distant regions. These considerations *Sketch of the Geology of Canada. Paris, 1855. TGeol. and Nat. Hist. Survey of Canada, Ann. Rpt. 1885, p. 12CC. —-. Lawson. ] The Eparchaan Interval. 53 were first clearly appreciated by James D. Dana, and in 1872 he proposed Archwan as a general term including the Laurentian, Huronian and other pre-Cambrian rock series which might or might not be the correlatives of these. The term \ \WZ@Z— Y gS 4 SINS 7 P4 Z Pate N\ = ‘2 , Chee Ss Qo" Mey, NX Z eens, . BERKELEY THE UNIVERSITY PRESS JUNE, 1902 PRICE 50 CENTS THE BULLETIN OF THE DEPARTMENT OF GEOLOGY OF THE UNIVERSITY OF CALI- FORNIA is issued at irregular intervals in the form of separate papers or memoirs, each embodying the results of research by some competent investigator in geological science. It is designed to have these made up into volumes of from 400 to 500 pages. The price per volume is placed at $3.50, including postage. The papers composing the volumes will be sent to subscribers in separate covers as soon as issued. The separate numbers may be purchased at the following prices from the University Librarian, J. = Rowell, to whom remittances should be addressed:— ee VOLUME 1. No. 1. The Geology of Carmelo Bay, by Andrew C. Lawson, with chemical analy- ‘ ses and codperation in the field, by Juan de la C. Posada : Price, 25¢ No. 2. The Soda-Rhyolite North of Berkeley, by Charles Palache - . Price, roc No. 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome Price, 4oc No. 4. The Post-Pliocene Diastrophism of the Coast of Southern California, by Andrew C. Lawson , Price, 4oc No. 5. The Lherzolite-Serpentine and Associated Rocks of the Potreo, San Francisco, by Charles Palache i gae No. 6. Ona Rock, from the Vicinity of Berkeley, ‘containing a New Soda Price, 30c Amphibole, by Charles Palache ; No. 7. The Geology of Angel Island, by F. Leslie Ransome, with a Note on the Radiolarian Chert from Angel Island and from Buri-buri Ridge, San Mateo County, California, by George Jennings Hinde 3 . Price, 45c No. 8. The Geomorphogeny of the ‘Coast of Northern California, by Andrew C. Lawson ‘ Price, 30c No. 9g. On Analcite Diabase from San Luis Obispo County, California, by Harold W. Fairbanks ; . Price, 25¢ No. 10. On Lawsonite, a New Rock- forming Mineral from the Tiburon Peninsula, Marin County, California, by F. Leslie Ransome . ‘ Price, roc No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte. Price, 20c No. 12. On Malignite, a Family of Basic, Plutonic, Orthoclase Rocks, Rich in Alka- lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, by Andrew C. Lawson : Price, 20c No. 13. Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene, near Berkeley, by John C. Merriam. : Price, roc No. 14. The Great Valley of ae a Criticism of the Theory of Isostasy, by F. Leslie Ransome . a Price, 45¢ VOLUME 2. No. 1. The Geology of Point Sal, By Harold W. Fairbanks . Price, 65c No. 2. On Some Pliocene Ostracoda from near Berkeley, by Frederick Chap- man . Price, Icc No. 3. Note on Two Tertiary Faunas from the Rocks of the Southern Coast of Vancouver Island, by J.C. Merriam . . Price, roc No. 4. The Distribution of the Neocene Sea-urchins of Middle ‘California, and Its Bearing on the Classification of the Neocene Formations, by John Cc. Merriam 3 f 4 Price, Toc No. 5. The Geology of Point Reyes Peninsula, by F.M. Anderson . . Price, 25¢ No. 6. Some Aspects of Erosion in Relation to the Theory of the Peneplain, by W. S. Tangier Smith : Price, 20c INO. 97. As Topographic Study of ‘the Islands of Southern California, by W. S. Tangier Smith . Price, 4oc No. 8. The Geology of the Central Portion of the Isthmus of Panama, by Oscar H. Hershey . : Price, 30c No. 9. A Contribution to the Geology of the John Day Basin, by John C. Merriam Price, 35¢ No. 10. Mineralogical Notes, by Arthur S. Eakle : 5 Price, roc No. 11. Contributions to the Mineralogy of California, by Walter C. Blasdale Price, 5c No. 12. The Berkeley Hills. A Detail of Coast SRE Geology, by Andrew C. Law- son and Charles Palache _ ‘ 8 4 F . Price, 80c _ UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 4, pp. 63=108. Pls. 5=16. ANDREW C. LAWSON, Editor TRIASSIC ICHTHYOPTERYGIA FROM CALIFORNIA AND NEVADA. BY JOHN C. MERRIAM. CONTENTS. Miraitete © CEG Ul © Tn tes ee te cen es eases dacs coh ay aut nde ecanesapanee todet ou ceeosertaseczize usntalasasshetss 63 Forms from Upper Triassie of Northern California, Bhestacaume group.... 65 OCCUNTONC Oi Pee eee ee ccs cess setadts enecue sess eee eee ees ee eee 65 Characteristics of Shastasaurus ..............--.-c---ceccee cceecees ceeeecteeeecceee ceeeeeeces cr ceeeres 69 NYEGROUEY ob EE SNEEE Wn aC Le] S10 ee ee Ce eee 69 JNTRGLOVE ISS ey eet ee ee oar oe a er re eee Re 0) HES cUT OTD GIO Sees ete eae pene fe oy ec cvs ans Sel Ses nte su anctel weci.cqhiceesec tebe cnden Gas ccvapicecnerae env oaeleae 79 CSU U ll SP ee ee eg a 84 HID) ern Hit NOM ete chee ee ae Fae ees e csc reduc sea sues eecssemeataneeceeae easel eae eeeecneseteee cv evets de 85 Aimitiesvamd Classiticablowl <.cc.cccccceccs.ce- tcsceeoceeeeee ove deeacs sedeea tecercesenaceeeceeesecacep 85 Dis traloubrom sam GS iy OMI... .2-.-.ces-sc8-s---0-+ -c-sce-e05e o-ceeeseee se -ecsneeteceoeseee eeeeeceaacs 87 IDGSCHIpPLOM"O LAS POCIOS ee.t, g.scre ac cedec sccrezecace sadeusct acseasst suesdauees sonqupesseeeseees ree 89 Shastasaurus perrini n. sp. ............... Be eS elec ceed ee sere cen 89 ie OSTMO WUE Weis Peyeenececee. teeceeereeeeee- SE es nies ee eee eee 93 M. allemam dae ans Sp vee eck sae cccececeer.z2cceeaceneeaeeeetee Pen dl 96 y CATO VALE TNS Perens ee nea eee Mores acu Jase paca ees ne ements ON GONE 2 98 de all CASO LEUULS SMES Pay see cs Nee ce ota tence tt rec mpm ect cs ees wy, zd POAC WC US NOTIN sy eceessteaee eee c secs oe se ees oes eee eee ear ee 102 Forms from Middle Triassie of Nevada, (Craitospondeine PTLOUPe eee OD Cymbospondylus Leidy ... opti tseTE ay taeee ee eee ee OS. Cymbospondylus piscosus cay Beer ee Seg caer sec oy sa oe Sere cee eee 104 H DO LRIMUS eC yee eee ee ee ee 105 2 FER CEE a0 WES} (=U by eee nee ee eae eee eee eee 106 eArtHiMableS#Ony OVO OSp ONY US! 2. cecreeee-cee-cseeeeecceezty nee ese sees ts oeeese-eeeeseenseeesteeeseeeee 107 HES ID 1 S142 YO EnV ee eee ssw ca ae ee ae Rte wame saa Seco say edanycSve nei ca tees ceccaev cucu serd reuse caseceit'seees 108 INTRODUCTION. In the spring of 1895, the writer received from Professor James Perrin Smith of Stanford University a number of vertebree and limb bones collected by him in the Triassic of Shasta County, California. In the same year, these remains were deseribed and figured under the name of Shastasaurus pacificus 64 University of California. [Von. 3 (Merriam, 1895). The genus was stated to have its closest affinities with the.Ichthyosauria but to differ in some important particulars from all known forms in that group. During the summer of 1901, the writer visited the Triassic areas of Shasta County in company with Professor Smith and a party of students from Stanford and California universities. On this expedition a considerable quantity of new material was obtained. In the fall of 1901, Miss A. M. Alexander generously contributed funds for another expedition into the Shasta region.’ Under the direction of Mr. H. W. Furlong, this party spent two months in the field and obtained some very valuable specimens. In working up these collections, it was found necessary to com- pare the Californian material with that which had been described from the Triassic of Nevada by Dr. Joseph Leidy, and through the kindness of Dr. Charles R. Kastman the type specimens of Leidy’s species were obtained for study from the Whitney collec- tion at Harvard University. In examining’ them it was discovered that Leidy had overlooked the most important characters of the species which they represent. The writer has, therefore, included in this paper a redeseription of the known Nevada forms. Practically all of the saurian material that is known to have been collected in the Triassic of this coast has been brought together in preparing the following discussion. Forms which are not recognized as representatives of the Ichthyopterygia are reserved for deseription in a later paper. For the present, two groups of species are recognized, those generically identical with Shastasaurus, from the upper Triassic of Northern California; and the middle Triassic forms from Nevada, which are all included in Cymbospondylus Leidy. These genera are probably closely related and form a well defined subdivision of the Ichthyopterygia. As yet but little is known concerning the structure of Cymbospondylus, while Shastasaurus is repre- sented by specimens showing’ nearly all of the skeleton, so that the principal discussion of the structure and affinities of this group naturally falls in the description of the better known genus. For the preparation of the drawings used in illustrating this paper, the writer is much indebted to Mr. Raymond Carter The photographs were all taken by Mr. B. F. White. Merriam] Triassic Ichthyopterygia. 65 FORMS FROM UPPER TRIASSIC OF NORTHERN CALIFORNIA, SHASTASAURUS GROUP. OCCURRENCE. All of the saurian material which has so far been discovered in the Shasta region has been found in two limestone areas lying in the northern part of the county. Most of the specimens have been obtained from a large area between Squaw Creek and Pitt River, a few miles north of Winthrop Post Office. It was in this region that Professor Smith made the first discovery of saurian remains in, 1893. b > a. The two varieties differ in color, intensity of pleochroism, and absorbtion, and the double refraction is a little stronger in the light than in the dark variety. The angle of extinction is the same for both, averaging 16°, and the direction of extinction being nearly at right angles to the transverse parting on (101). Twinning is frequent on (100), the two main divisions of a twin often showing three or four twinned lamellae between them. In sections cut parallel to (010), this twinning causes with the parting on (101) a faint “herring bone” structure similar to that shown by augite. The two varieties of hornblende are crystallized in perfect continuity with each other. Sometimes the dark mineral is the center of a erystal; sometimes the hght forms the neucleus. In general it may be said, however, that the dark green variety is 178 University of California. [Vou. 3. the older and probably the more basie form, as in the majority of cases the light mineral is moulded around it. The minerals included in the hornblende are magnetite in irregular grains and well-formed erystals, and apatite in small prisms. Some secondary epidote, with its very high birefring- ence, has been formed, as well as some chlorite. |The epidote is often interlocked with fibers of undecomposed hornblende in an intricate manner. The feldspars under the microscope are very clear, and in most cases free from secondary products. What appears to be single erystals to the unaided eve are found to consist of a number of smaller individuals, with a few traces of idiomorphie boundaries. In size the erystals range from 3.09 mm. at a maximum to less than 1 mm., averaging 1.10 mm. Cleavages parallel to base and brachypinacoid are developed sparingly. The twinning most commonly observed is that on the albite law; often pericline lamellae are seen, and more rarely carlsbad twins. The measurement of the maximum symmetrical extinction angles on the albite lamellae indicate that the feldspars range from andesine, with an extinction angle of 20°, to a medium basic labradorite, with an extinction angle of 412. However, most of the feldspar corresponds to an acid labradorite, with an extinction angle of 35° This determination of the feldspars was checked by specifie gravity tests, using Klein’s solution. MINBRALS >. ; ae Be ae FROM Vina ei LEONA HEIGHTS ALAMEDA €0., CALIFORNIA : : Jp! ‘ he WALDEMAR T. SCHALLER i ra ba " i! a “¥ oft i be : : Bk ig A Bo oy ; hwy ae v fe - 2 “ COOL. ; 7 cae. Y » : t ~ us t; of ; ay %, sl dp me, ‘ A \ rye | ; Wy * ; ea Py ? y } ) 4 bat « Z . ie 4. By HY A Y 5 ae eae Peas IZ Were 72h me is) SSS \ Betas é 3 y S< = Z 3 7 >) 4 gS 7 2 1-4, GINS ZF et ae . x, IN\Nenne eS eto. SR A, +O! Y/f\\\ A Pees WE 4) | EA wi Ree TE Sie a Pens my. Ny =o / ita itm ~ ey, C4 Nye Sy ye 4 ‘ * me, r home Ot SST EB ‘ai oS Per ewreeyeeesOee™ *e, be BERKELEY THE UNIVERSITY PRESS ine APRIL, 1903 PR CG ic, \ & PRICE 15 CENTS » \ a i : , 4 A \ FORNIA is issued at irregular intervals in the form of sepatae papers or ree a : { embodying the resul{s of research by some competent investigator in,geological science : y It is designed to haye these made up into volumes of from 400 to 500 pages. The ‘price per volume is placed at $3.50, including postage. The papers composing the volumes” if { will be sent to subscribers in separate covers as soon as issued. The separate numbers ie _ may be purchased at the following prices | from the University sia Nip, Gs oes to Aw Ror! , whom remittances should be addressed:— - ¢ ? ee Py “VOLUME iy yeaa A age yin No. 1. The Geology of Carmelo Bay, by Andrew C. wson, with chemical arialy r ms ses and codperation in the field, by Juan de la C. Posada : Price, 25¢ No. 2. The Soda-Rhyolite North of Berkeley, 1 Charles Palache , .) Brite aroc No. 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome |. ig PACES AOC ais No. 4. The Post-Pliocene Diastrophism of the Coast of Southern California, by } ih i Andrew C. Lawson : . | Price, 4oc No. 5. The Lherzolite-Serpentine and Associated Rocks of the Potreo, San) tnone. Francisco, by Charles Palache je eta ‘ No. 6. Ona Rock, from the Vicinity of Berkeley, ‘containing a New Soda ( y: Amphibole, by Charles Palache : BueGroce Bb No. 7. The Geology of Angel Island, by F. Leslie Ransome, ‘with a Note on the Radiolarian Chert from Angel Island and from Buri-buri* Ridge, San i : Mateo County, California, by George Jennings Hinde 5 . _ Price, 45¢ No. 8. The Geomorphogeny of the ‘Coast of Northern California, by Andrew Cc wt Lawson : Price, 30c No. g. On Analcite Diabase from San Luis! Obi o County, California, by Harold W. Fairbanks : . Price, 25¢ No. 10. On Lawsonite, a New Rock- forming Mineral from) the Tiburon Peninsula, ‘ { Marin County, California, by F. Leslie. Rarediie : Price, roc Bash No. 11. Critical Periods in the History of the Earth, by Joseph LeConte . Price, 20c No. 12, On Malignite, a Family of Basic, Plutonic, Orthoclase Rocks, Rich in Alka- : lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, a y pad by Andrew C. Lawson. é, Price, 20¢ No. 13. Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene; near va Berkeley, by John C. Merriam. . Price,toc “ No. 14. The Great Valley of epee a Criticism of the Theory of Isostasy, by : oy F. Leslie Ransome . on ood a MYO Meee 45¢ if Gy ie aes, VOLUME 2. oa No. 1. The Geology of Point Sal, By Harold W. Fairbanks “ . Price; 65¢ ni alee No. 2. On Some Pliocene Ostracoda ee near, Berkeley, by Frederick Chap- a man . Price) JGCi sion 7 ame _ No. 3. Note on Two Tertiary Faunas ineth the Rocks ‘of the Southern Coast of ee "pi Vancouver Island, by J.C. Merriam . . .. Price, toe, ? No. 4. The Distribution of the Neocene Sea-urchins of Middle California, and Its Bearing on the Classification of the Neocene Formations, by John Cc. Ms Merriam : : sae Price, I roc y; No. 5. The Geology of Point. Reyes Peninsula, by 1, M. Anderson .. \,. Price, 25¢ No. 6, Some Aspects of Erosion in Relation to the Theory of the Peneplain, by | W. S. Tangier Smith 4 Price, 20c No. 7. A Topographic Study of ‘the Islands of, Southern California, ‘by W. S. Tangier Smith : Price, 4oc No. 8, The Geology of the Centtal Portion of ‘the Isthmus of Panama, by Oscar H. — s Hershey .. : Price, 30c INO: 99.02 Conaabition to the eesigny of the John Day Basin, by John c Mena | rice, 35C pi ; No. 10. Mineralogical Notes, by Arthur S. Hakle K i Price, roc- * j No. 11. Contributions to the Mineralogy of California, by Walter C. Blasdale Price, 15¢ No. 12. The Berkeley Hills. A Detail of Coast Range Geology, by Andrew C. Law-. d son and Charles Palache 5 : E hist te 4 Pie Price, 8oc UNIVERSITY OF CALIFORNIA PUBLICATIONS : Bulletin of the Department of Geology Vol. 3, No. 7, pp. 191=217, Pl. 19 ANDREW C. LAWSON, Editor MINERALS FROM LEONA HEIGHTS, ALAMEDA CO., CALIFORNIA BY WALDEMAR ,. SCHALLER CONTENTS PAGE Unt RO CUCU OMe cer escetr cet, yetereens oe coco en wher nO RE oe 192 Mla ritO rss. sare sea eas Aire ee ie pO ey Oe 193 General@Descrip tine... sinc aceon ete Ce sabe on. ee Mien a 193 Crystallographie Characters... Pedic: Br SPR ty crit eee 1B i ’ Chemicalbbropenticsss este erat ye ees 194 Chaleopyrite QUO) DY ENE ere a ace ee ~ Melanterite Generale D escrip tiomesseete tte etl eevee ete ces cee. FOES). ch eat eke PO), OE 195 Crystallographie Characters Physical Properties (Claneraaiepnll TEA oy XE AOU ve ees 5 eee ee ete aE OU oe tae oa 198 — ilspatllig Kea cs Bere el Sr ee ee 199 ConenaleD OSCrip tion mers amen. Mek ee Se ie bee 199 Crystallographic Characters ....00.00. 02.0. eeceeeee e 199 ey SiG alll TOP OLtUCS i: ce fak. ee ceecs oeoerecce Gisecevaes cst sadeeese sseaeeeee Sa ee eres es “CLS 28 Oy 0X9 1S es RE | Uae ee ee 204 STRAT LHS) ces ee ee? 7 General Description 00... 000 eee Aetebnctel Nees stye ee ame a re tM OE 207 Crystallographic Characters 00.00... ..cccccccccccecccescece ceeeees ce ceseeeve eeeeereeeeeens seers. 208 Why SiCaWPLOPOTtISS! j.c.-.c..20 aeectececc a ceecsedece ceeeeee eoeetes 210 Chemical) Properties... 2 sees cece eeeeeee tee eee ee 210 ba Chia camthiit ope tire tes er es) cet ck te OIE, Bice i eccyctibdiceson igcucaseceeee 212 General Description 0.0.0.0... 0... 212 Crystallooeraphic Characters... cec:.2 ele seecece seecsseeseceees ce Oe ane ape be _ Chemical Properties ........ KCopiapite.c4, .-..0ne- rem enallw) Gs Cui bl ON eseree tee ey cee eee ee eee ay es eee esse. cee O14: @hemicallMeropertics:: 240.5 ere Sa eS Agee tesco teens ac es eee ea 214 Mipsomile pete went ee Meee re met ae SF WN htt oi Ne 216 General Description lve mic HMOT OD CTUNCS:sspemp estate fg nese roe encanta ee, 26 aSAVIIN OG OTe free ee Ls: ~ Hematite and Limonite Summary 192 University of California. [Vor. 3. INTRODUCTION. A small body of pyrite occurs near Leona Heights, Ala- meda Co., Cal., containing some chalcopyrite, and the ore has been mined for a number of years for the manufacture of sul- phurie acid. In consequence of the oxidation of the sulphides, several secondary sulphates of iron and copper have been formed in and about the mine, and specimens of these secondary minerals have been collected and studied by the writer. These natural vitriols occur in such good crystals that an interesting crystallographic study can be made of them. Our present crystallographic knowledge of these sulphates has been largely dependent on the study of artificial crystals. All of the minerals found at this locality, with one exception, were identified with known species. These are Pyrite, Chalco- pyrite, Copper, Melanterite, Pisanite, Chaleanthite, Copiapite, Epsomite, Hematite, Limonite and Alunogen (?). Besides these, a copper sulphate with seven parts of water, Boothite, to be described later, was also observed. Of these pyrite, melanterite, pisanite, chaleanthite and boothite occur in good measurable crystals. Copiapite occurs, to some extent, in crystals, but they are all microscopic. The erystals were measured with the two-cirele goniometer, except a very few fragments, which were broken in such a manner as to render their setting up in true polar position impossible. The forms on these fragments were, consequently, determined from measurement of the interfacial angles. While many of the faces gave excellent reflections, the ratios obtained from the two-cirele readings were, with one exception, not con- sidered as more accurate than those previously obtained. The one exception is pisanite, for which elements were calculated from the readings. These, it is thought, approximate more closely to the true elements than those which heretofore have been accepted for pisanite. In the chemical analyses the iron was determined by titration with potassium permanganate, with occasional checks by weigh- ing the iron as ferrie oxide. The copper was determined by iodometric titration. The water was weighed directly in a ScHauurr. | Minerals from Leona Heights. 198 ealeium chloride tube, fractional water determinations being’ usually made. It was found, by experiment, that all of the ® “ « e) water of these sulphates was given off below 800° C. PYRITE, General Description.—The ore of the Alma Mine consists chiefly of massive pyrite intermixed with some chalcopyrite and usually carrying small values of gold and silver. Crystals of pyrite oceur scattered through the rock, which is rhyolite, often largely decomposed to clay. The crystals described here, were collected some years ago at the opening of the mine by Mr. Fritz Bohmer, of Alameda, who kindly placed them at the disposal of the writer. Crystallographic Characters.—On examination with the lens, the crystals, ranging up to 8mm. in diameter, and even occasion- ally somewhat larger, were found to consist principally of the pyritohedron }120{, with occasionally the cube and the octo- hedron. The cube faces are invariably narrow and the octahedral faces triangular in shape, the latter varying in size up to about one-third the size of the pyritohedron }120{. All of the larger crystals are more or less rounded and the faces uneven and often dented, always giving a large number of reflections. The ten forms below were definitely established and a few more possibly are present, but on account of the lack of sharpness of the signals, their identification is somewhat uncertain. Letter. Symbol. Letter. Symbol. Gat. Miller. Gdt. Miller. a 0x 100 0 ] itl d we) 110 w 13 252 8 a 4 340 n 12 121 e 2 2 120 t 24 241 h n4 140 s 23 231 The forms $100}, 3}110{, }340{ and }140( occur as narrow and rounded faces. Of the other forms only }120( and }111 were well developed. The remainder were all small and the complete number of faces belonging to each form was not always present. 194 University of California. [Vor. 3. The following table shows the measurements together with the calculated angles for these forms. a Symbol. | Measured, Calculated. No.| # — 4) Gat. “Miller. | co) p | © p ae || | as ines ame 1 | a 0% 100 | 0°00’ 90°00’ 9°00" | 90°00" 2} d| o | 110 || 4454) “ | 4500) “ 3|8 | o4 | 340 || 37 01 ce 36 52 os 4] e a0 2, 120 26 30 ee 26 34 My 5!Ih w4 140 14 12 Le 14 02 Ye 6 | 0 1 111 45 12) 54.45 | 45 00 | 54 44 _ re ong || {46 36 ; 29 31 29 30 “| @) *2 | #98 |) 90 46 | 71 24 | 91 48:1 69 37 eee eee yoy | {44 45 33 46 | 45 00 | 35 16 /} 126 28 | 6610 | 26 34 | 65 54 | (14 20 | 64 52 | 14 02 | 64 07 (26 15 | 7 1'93 45 | 8 s| 23 | 231 |l418 38 | 5 | | (33 46 | 7 The combinations of forms on the measured erystals are shown in the following table: Cryst. g @ § € h o wn ts 1 ¢ 7) n 2 a—-—ehiow—n— s 3 adsbeh own t's 4 a—-—e—o gant s 5 ad§ée—o oan — 8s Chemical Properties.—Chemical tests showed that the erystals of pyrite contained no copper. The massive ore, however, gave a reaction for copper, which probably comes from the admixed chalcopyrite. Other elements, such as arsenic or thallium were not tested for. CHALCOPYRITE. Some portions of the massive ore show a sulphide having the color of chalcopyrite and affording a qualitative test for copper. No crystals of chalcopyrite were met with; neither were any large masses of pure chalcopyrite found. SCHALLER. | Minerals from Leona Heights. 195 COPPER. Native copper occurs very sparingly in a shaft sunk some distanee above the Alma Mine, as small arborescent groups con- sisting of irregularly grouped, distorted erystals, possibly octa- hedrons. MELANTERITE. General Description. — The ferrous sulphate, melanterite, oceurs rather widely distributed as an efflorescence, but only in small quantities. In the mine it occurs as small prismatic crys- tals, up to 2 mm. insize. : PISANITE. General Description.—The most 28 oundant secondary mineral occurring in the mine is pisanite. Long prisms of this mineral are seen almost everywhere and large magnificent specimens are rather abundant, especially near the mouth of the northern tun- nel. Unfortunately, on the shehtest jarring most of the crystals readily detach themselves from the rock. Many of the crystals seem to have formed directly on the rock and were lying loose; unattached. Others again were feebly united to the rock, especially at one end of the prisms and these hung down- ward in large groups. No radial or other regular grouping of the erystals was observed. The specimens are quite free from other minerals, the conditions, at the time of formation of the crystals, seeming to have been just right for pisanite and not meght for any other mineral. The mineral probably erystallized out from a solution of iron and copper sulphates. Zonal structure, though common in the artificial crystals, was not observed in the natural ones. Inclusions of pyrite are not uncommon and drusy pyrite fre- quently covers the crystals to a large extent. Crystallographic Characters.—The erystals average about 5 mm. in length and about 1 mm. in thickness. Many are much longer and the thickest one measured 38 mm. by 4 mm. on the base. Certain crystals of pisanite had been partially dis- solved, the re-solution going on with a remarkable difference in * Inorganic Chemistry, by Ira Remsen, 5th edition, 1898, pp, 218, 709. 200 University of California. [Vou. 3. rapidity in different directions. Many of the crystals are hollow, the inside being entirely dissolved away. Occasionally portions of the prism faces are also dissolved, leaving merely shells. Hitherto, our knowledge of the erystallography of pisanite has been limited to the results obtained by Des Cloizeaux, who derived his elements from three interfacial angles. The method of measurement, with the two-circle goniometer is peculiarly well adapted for the determination of the axial elements since all of the readings can be used. From the average values of p’o, q’o and e’, and the readings on the prism faces, the following axial ratio was obtained by the writer: a@-b2¢ = 1.16702 1; 1.5195. 8 — 105-1 The ratio does not vary much from that obtained by Des Cloizeaux, namely: a:b:¢ =1.1609:1:1.5110; B = 105° 22’, but is believed to be nearer the true one. The erystals were readily adjusted in true polar position, as usually all four of the prism faces were present and all gave excellent reflections. In all, seventeen forms were observed, of which ten are new. These forms are given below in two columns, those in the second column being the new ones. Letter. Symbol. Letter. Symbol. Gat. Miller. Gdt. Miller. c 0 001 a wo) 100 b Qo 010 h 200 210 m 0 110 i 300 320 w +40 103 l oo 2 120 t —10 T01 v +10 101 7) 01 O11 g —20 205 T —3 1 r +1 111 iE —3 335 D 3 221 o —12 121 The angles measured, together with those calculated from the elements obtained by the writer, for the forms, are given in the table below. SCHALLER. | Minerals from Leona Heights. 201 = ; os A Syinbol. | Measured. Caleulated. ~| 3 | Gat. |Miler.|| p | p 1 c 0 | 001 |} 90° 00’| 15° 11’| 90° 00’| 15° 11’ 2 b oS 0 | 010 0 02 | 90 00; O 00 | 90 00 3 | a oo () 100 89 32 ue | 90 00 2 | h | 20 | 210 || 60 25; *” |60 37} ” 5 |- f | $0 | 3820 || 53 26 ” 53 06 ” 6] m | | 110} 41 36) ” | 41 1 ” Tale) co) W120) 9/223; 945 n | 23 56 ” 8/ w | +40 | 103 | 90 00.; 36 00/90 00/35 48 9| v | +10] 101 |} 90 02/58 12 » 158 19 10| g | —30 | 205 ||/90 03/15 00/ ” | 15 O01 11 | t —10 T01 90 02 | 47 13 | ay 47 09 12 | o 01 011 || 10 28 | 57 oe 07 | 57 04 13 | r | +1 | 111 ||46 43); 65 35/46 50/65 46 14] 7 | —3 | T12 | 27 22) 40 21/27 57] 40 42 15 | E | —% | 335 | 30 28) 46 28] 30 33) 46 38 16/ p | —2 | 321 '|39 04/75 25|38 37/75 35 eG 108 Oe EO eA O72 25 1195. 32 972" 46 The following are the new forms, briefly described: a = 00 = 3100}. The orthopinacoid was noted twice, once as a broad face and once as a narrow face. h =2e% = 3210}. This prism was noted on three crystals, as rather large faces. f = 3m = $320}. On erystal No. 1 was noted a small face in the prism zone, the measurement of which agrees well with the caleulated value, though the reflection was very poor. 1 = ©2= 3120}. This prism always occurred with h, and was about equal to it in size. Crystal No. 15 showed the three new forms, a, h and J, in the prism zone. v = +10 = }101}. Only once was this form noticed, as a small face with a poor reflection. g = —30 = 3205}. This dome also occurred but once as a rather large face. It gave a good reflection. yr =+1= 111. The unit pyramid was represented by a long narrow face, giving a good reflection. 202 University of California. [Vou. 3. E= —? = $335}. This form was noted but once as a long narrow face. The face is in the zone ¢ m. D= —2 = }221. This form occurs on two erystals. The reflections in both cases were fair. o = —12 = }121{. = — 14 —— hy — 15 e—ah—m 1 o 16 m — to-—-—-—-—--—-— Ef c a m v All of the forms observed by Des Cloizeaux were noted on these crystals, except —$ = $889} and — sy = {5.5.22}, which are probably vicinal. In the following table the values are derived from the measurements by the writer, and show a slight difference from those given by Goldschmidt: SCHALLER. | Minerals from Leona Heights. 203 a 1.1670 lga 0.06707 | lg ao 9.88537 lg po = 0.11464 ao = 0.7680) po = 1.8021 e 1.5195 Ige 0.18170 lg bo 9.81830 lg qo 0.16628 bo = 0.6581 go 1.4665 B= is Vagogg = Vo ogis7!®°= Lo gigtalig 22 = 9.94836 h = 0.9651 | ¢ = 0.2619 180 — BS lg sin po J Ig cos bh j a0 | | Peder *. "ai | | a’ S|: rf 7 a’ g/ 2 eis p p & No é H | (Prism)) a Pa ys 5 | a | (w:y) BP | reel teal vizio a lamom ari maein atin Beal aneia ailin ap ees | Ae 1] e¢ |} 0 001//90° 00')15° 11 J15°11’| 0°00//15° 11’) 0° 000.2714] 0 |0.2714 2b 0% 010 0 00.90 00 0 00.90 00 0.009000, 0 % | ® 3 | a | 0 100,90 00 “© (90 00) 0 00.90 00.000) «% | 0 | « 4 | h | 200 |210||60 37] ‘ * 190° 00/60" 37 |29°23)1.7758) co | ** 5 | f |$oo [320/153 o6| -«* | * | 153 o6|36 54/1.9319| “ | « 6 | m| o /110|/\41 36] ‘“* ue ‘* J41 36/48 24/0.8879] ee 7 || w2\120/93 56] “ | * «“ log 56/66 04/0.4440) “ | « 8 | w |+40/103|'90 00/35 48/35 48] 0 00|35 48| 0 00\0.7211) 0 0.7211 9 | » |+10/101]} ‘* (58 19/58 19] ‘* [58 19) ‘* |1.6206| ‘‘ /1.6206 10 | g |—20)205)/90 00|15 01\T5 01| ‘* [15 o1| “ |0.2683) ‘* |0.2683 11 | ¢ |—10/T01]) ‘* 47 09/47 09) ‘* [47 09; ‘* |T.o778; ‘* 1.0778 12 | 0 | 01)/011|/10 07-157 04/15 11|56 39} 8 29|55 42°|0.2714!1.5196|1.5436 65 46/58 19] ‘ [41 42/38 35/1.6206 1.5196/2.2215 13 | » |+1 {111/46 50- 14 | w |—$ |T12)27 57-40 42 21 58/387 13°17 48/35 10 | 0.4032 0.7598 0.8602 15 | £ |—2 [335/30 33/46 38/38 17/42 21:31 41/38 45:|0.5381 '0.9117/1.0587 16 | » |—2 [221/138 37/75 35 67 36-71 47 37 11 149 11 | 2.4270 3.0392 3.8890 17 | o |—12/121||T9 32/72 46/47 09) ‘* {I8 37/64 11|1.0778,; ‘* [3.2245 Physical Properties.—The plane of symmetry is also the plane of the optic axes. A section of the mineral cut’ approxi- mately parallel to the chnopinacoid showed that the axis of elasticity nearly parallel to the eclino-axis was the axis of mini- mum elasticity. A seetion cut normal to this axis of elasticity, showed, in convergent light, a biaxial interference figure with a large angle. This figure also showed its positive character. SS i) eb an — Mh = — — 7 ss — 6 CON AE eg wy ps 7 Oe ae et TT p zg The following table gives a caleulation of the two new forms, (170) andig — 714103 g “| H | x a’ Fe | co) p & No | S 7 |(Prism) y’ si s8lea|s | =tep 4ZlH| o/Aa | (ay) l ee | Paar a ie : 7 | 1| 7 | 2 (1201 37° 14’ 90° 00’ 90 00'90° 00’ 37° 14’52° 46" 0.7601 & oo 2g | 14 /141/)140 45 |64 23 52 5058 14.34 47 44 17 RHE GE) 2.0851 | | | : Chemical Properties.—All of the analyses showed merely a trace of magnesia, and no iron. The erystals represent, there- fore, a rather pure copper sulphate. The average of the analyses gave: 214 University of California. LVon. 3. Analysis. Ratio. CuO 31.14 .97 FeO none MgO trace SO; 32.06 1.00 H20 (110°) 28.20 NN aye H2O (above 110°) 7.50 Ye Insol. 81 99.71 Considering, as before, that the water given off at 110° is water of erystallization, while the remaining molecule is consti- tutional water, we may write the formula of chaleanthite, J ore ee oo cu CuSO4.H20+-4H20, or structurally, OS < 6 +4420. \ o> He This formula differs from that of boothite only in the fact that it has four molecules of water of crystallization, instead of six. COPIAPITE. General Description.—A yellow ferric sulphate is quite abun- dant, both at the mine and in the immediate neighborhood, which agrees well in its various properties with copiapite. Some distance from the mine, on what is probably an old prospecting dump, a thick layer of copiapite occurs which was selected for the analyses. Some distinct, though microscopic erystals, occur associated with pisanite, but the entire amount of this material is too small for a chemical analysis. Under the microscope, with the highest power, the minute crystals are seen to be six-sided tabular erystals, nearly colorless and nonpleochroic if thin, but somewhat pleochroic if rather thick. The pleochroism is colorless to pale yellow. Cleavage is perfect parallel to the plates, which are probably copiapite crystals tabular to the clinopinacoid. They are too small to show the emergence of a bisectrix. Chemical Properties.—Under the microscope the material analysed was seen to consist of a granular mass with no distinct crystals, with which a few colorless prisms were intermixed. Some of these prisms give parallel extinction and are probably epsomite while others give varying angles of extinction up to SCHALLER. ] Minerals from Leona Heights. 2115 about 20° and were possibly melanterite. The amounts of fer- rous iron, magnesia and alumina varied somewhat in different samples. The average of several analyses of this material gave the following results: Analysis. Ratio. Fe.03 25.04 15.65 AloOs O31 0.30 ey, FeO 0.44 0.61 / MgO 0.29 0.73 SO; 38.36 47.95 aie) HO 29.71 165:06 | Insol. 5.43 99.58 A fractional determination of the water gave: HO (at 110°) 20.25 ” (at 150°) 300) ” (at 200°) 2.26 ” (at 260°) 1.77 ” (above 260°) 2.33 29.71 These water determinations were not carried out very accur- ately but they show that about two-thirds of the water is given off at 110°. To assume that exactly two-thirds or 12 molecules of the water are given off at 110°, which is probably water of crystallization, would give us, for the formula of copiapite, 2Fe203.5803.6H20+12H20. If, now to obtain the acid of which copiapite is the ferric salt, we substitute for Fe” its equivalence 3H, we obtain 2(3H)203.5503;.6H20+12H20. Neglecting the twelve molecules of water of crystallization, and ‘reducing the first part of the formula, we obtain 6H2O0.5S0O3 6H2O=5H2SO4.7H20 as the acid from which copiapite is derived —a very improbable acid. If, however, we assume that fourteen molecules of the water, instead of twelve, are water of crystallization, we then have 2Fe203. 5803.4H20+14H20. as a formula for copiapite. Again substi- tuting 3H for Fe”’, this becomes 6H20.5SO3.4H20+ 14H20., or, neglecting the fourteen molecules of water, 2H2O.SO3 = H2SOg. HO, which latter is tetrahydroxyl sulphuric acid, as the acid of which ecopiapite is the ferric salt. This formula would require 216 University of California. [Vou. 3. that 24.2 per cent. of water be given off at the first temperature, about 110° Structurally, the formula for copiapite would then become, | oO = 4 | OS OS : | EPSOMITE. General Description.—Epsomite occurs in the mine, and was also frequently observed in the immediate vicinity, as an efflores- cence. It occurs as bent and curved fibrous prisms, showing, however, no crystal surfaces. Under the microscope the prisms give straight extinction. Chemical Properties.—The analysis served merely to identify the mineral. Analysis. Insol. deducted. Caleulated. MgO 12.4 14.8 16.3 SO; 26.5 31.7 32.5 H20 (110°) 34.1 40.8 aire HO (above 110°) 10.2 12.2 hon Z Insol. WB cn Al,O3 trace trace FeO ) ante) j Poe rc. 99.5 99.5 100.0 The formula for epsomite may be written, like that of eon / DME melanterite, O84 6 +6H,0. sh ALUNOGEN. A coating of white powder, intimately associated with pieces of copper sulphate, covers the bunkers in front of the mine. The powder is readily soluble in cold water, which solution gave tests for copper from the admixed copper sulphate, aluminum, sulphuric acid and water, with traces of ferrous iron and magnesia. Under the microscope the mass consists of a granular aggregate of a white mineral, only partially transparent. The mineral agrees, so far as can be SCHALLER. ] Minerals from feona Heights. 217 determined, with alunogen, and is tentatively referred to that species. Besides the efflorescences of epsomite in the neighborhood, an occasional specimen was met with which, besides giving a test for magnesia, showed also the presence of aluminum in fairly large quantities. It is probably a mixture of alunogen and epsomite. All of the specimens were, however, impure and dehydrated to some extent, so that no analysis was made of any of these aluminium sulphates. HEMATITE AND LIMONITE. The alteration of pyrite is usually accompanied by the forma- tion of oxides of iron, and both hematite and lmonite occur at the mine. The hematite is in the form of a compact red ochre. A specimen gave 10 per cent. of water, which may have been occluded, or the mineral may be classed as turgite. The hmonite occurs mostly as yellow ochre, although occasionally it is in compact brown masses. SUMMARY. By the study of the sulphate erystals formed by the oxidation of the pyrite ore, ten new forms are established for pisanite, seven for melanterite and two for chaleanthite. A new sulphate of copper containing seven molecules of water, instead of five, occurs as one of the secondary minerals, to which the writer gives the name boothite. The three minerals,, pisa- nite, melanterite and boothite form an isomorphous series. The theory is advanced that all of these hydrous sulphates may be regarded as salts of tetrahydroxy] sulphuric acid, since they apparently contain one molecule of constitutional water. In econelusion, the writer wishes to express his thanks to Dr. Arthur S. Eakle, under whose guidance the investigations were carried out. Also to Dr. W. C. Blasdale and Mr. Booth of the Chemical Department, and to Mr. Storch, the superin- tendent of the pyrite mine, grateful acknowledgements are due, for much assistance. University of California, April, 1903. - 8 ™ Bulletin of the 2 Department of Kiersey ; ak Bees 3 No. 8, » PP. 219-229. aha ha ry it i ANDREW C. LAWSON, Editor ‘ NEAR SPANISH PEAK, CALIFORNIA. BY al ANDREW C. LAWSON , eorenes2aneags, eg iS Cay : ae <= Wie Lo = XO Y} Y » Nyy irra) Pare eerweee Se -BERKELEY THE UNIVERSITY PRESS APRIL, 1903 PRICE 10 CENTS . THE BULLETIN OF THE DEPARTMENT OF GEOLOGY OF THE UNIVERSITY ¢ FORNIA is issued at irregular intervals in the form of separate papers or memoi ri embodying the results of research by some competent investigator in geological sci It is designed to have these made up into volumes of from 400 to 500 pages. ‘The p per volunie is placed at $3.50, including postage. ‘The papers composing the volumes will be sent to subscribers in separate covers as soon as issued. The separate numbers , ey be purchased at the following prices from the University Librarian, NBS Reet to i whom remittances Sage be addressed: — ve VOLUME 1. © : Hi Pe P., No. 1. The Geology of Carmelo Bay, by Andrew C. Lawson, with chemical analy-— may ses and codperation in the field, by Juan de la C. Posada J Pricey 25C No. 2, The Soda-Rhyolite North of Berkeley, By Charles Palache J) he eBaiges LLOQ tas No. 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome 5 Price 4oc No. 4. The Post-Pliocene DiastrophHism of the Coast of Southern Califernia, by _ - Andrew C. Lawson ; : ‘Price, 4oc Saye No. 5. The Lherzolite-Serpentine and Associated Rocks of the Bancos San Peat ete Ai Francisco, by Charles Palache 4 caves re & No. 6. Ona Rock, from the Vicinity of Berkeley, ‘containing a New Soda (P : c me Amphibole, by Charles Palache : pie ge ee No. 7. The Geology of Angel Island, by F. Leslie Ransome, ‘with a Note on the Radiolarian Chert from Angel Island and from Buri-buri Ridge, San Mateo County, California, by George Jennings Hinde y i eces 4B cn a No. 8. The Geomorphogeny of the Coast of Northern California, by Andrew Cc Lawson A Price, th, No. 9. On Analcite Diabase from San Luis Obispo County, California, by Harold — i “W.Fairbanks ~~ . 4\0 ) aPrice S25 cmsnam No. 10. On Lawsonite, a New Rock- Forming Mineral from the Tiburon Peninsula, vi Marin County, California, by F. Leslie Ransome . ia a Price arog ek No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte. Prige, aoc) ne No. 12, On Malignite, a Family of Basic, Plutonic, ‘Orthoclase Rocks, Rich in Alka- Marcd & Pint lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, ‘ by Andrew C. Lawson é (Price, 206 Tau No. 13. Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene, near — i Berkeley, by John C. Merriam. 7 3 Price, roc — No. 14. The Great Valley of California, a Criticism of the Theory of Isostasy, by F. Leslie fi geenals . ; ‘ ea : ‘Price, bia VOLUME" 2 ~ No. 1. The Geology of Point Sal, By Harold W. Fairbanks > oy Pricesio5e No. 2. On Some Pliocene Ostracoda from near Eons by Frederick Chap- Mia man . 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Contributions to the Mineralogy of California, by Walter (, Blasdale Price, 15¢ op No. 12. The Berkeley Hills. A Detail of Coast Range Geology, by Andrew C. Law- a ; son and Charles Palache . 5 ane a Rats BSR |b eee Soc wry UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 8, pp. 219-229. ANDREW C. LAWSON, Editor PLUMASITE AN OLIGOCLASE-CORUNDUM ROCK NEAR SPANISH PEAK, CALIFORNIA BY ANDREW C. LAWSON. CONTENTS. PAGE Recent Recognition of Corundiferous Roeks ........ forte SER eR NS) SADNGG) DMS EXONS eae rE ee i oy CEO oe eo 71 The Peridotite Cut by Corundiferous Dyke... .... i secre Ak toe Ae ROR OUe IE: 222 Chemical Composition of Peridotite 0... 0... ceeeeteeteeteeeeee oe came 224 Original Edenite....0.. 2 202... De ee aE ea ier a ee ee eee Lee 225 Extent of Corundiferous Dyke 000.0 2 oe. oe sa tesi ee 225 The Corundiferous Facies ......... 00... ees er a Sc Oe 225 The Corundum .............0. te Ree ee por a eR err, 5205 Ran Oy 226 Chemical Composition of the Rock... cece cece ce eect teens 227 He mo Clee Wy 6 eID CLC sx oe noes vleccect osc. seaseass scot ezincsshecakasdsGeeaceezewssecetcace . 227 Other Facies of the Dyke. 000. 0... Bee eee SO sce ees od, ee OS (Comanellaninkevatcse. 2 See eee Fe na ee erate a AT Te Rees or, 2 229 Recent Recognition of Corundiferous Rocks.—One of the notable features of petrographie research during the past few years has been the discovery in several widely separated portions of the earth’s surface of roeks in which the mineral corundum plays the réle of a normal constituent. The mineral has long been known as an interesting accessory in certain granite rocks and as a not uncommon occurrence in certain metamorphic schists and erystalline hmestones. But the interest attaching to these occurrences has been almost purely mineralogical, and they have contributed but little to petrological science. Even in the latest text-books corundiferous igneous rocks are not discussed. In the last edition of Iddings’ translation of Rosenbusch’s “Mikroskopische Physiographie,” 1898, it is asserted that 220 University of California. [Vor. 3. “corundum never occurs as an essential constituent of rocks, with the exception of emery, which, together with iron oxides, forms independent bodies in the erystalline schists. It appears only as an accessory constituent in granites, gneisses, granular limestones and dolomites, and is constantly accompanied by spinel, rutile and sillimanite.” In Rosenbusch’s last book, “Elemente der Gesteinslehre,” 1898, rocks of this interesting character are not recognized. These facts are not mentioned by way of eriticism of the text- books, but simply to emphasize the receney and_ practical simultaneity of the various discoveries referred to. These dis- coveries have, moreover, been supplemented, and, indeed, in a large measure anticipated, by the brilliant synthetic studies of Morozewiez.* In contrast to the state of knowledge at the date of the text- books above referred to we have to-day a considerable body of information -on the occurrence and character of corundiferous ioneous rocks. In India Holland? has described a corundum syenite. In Russia Morozewiez has described corundum syenite and corundum pegmatite from the Urals} as well as a more basic type consisting of anorthite and corundum together with some biotite with accessory spinel, apatite and zircon, to which he gives the name Kysehtymite. In Eastern Ontario, Canada, there have been discovered areas of corundiferous syenites, nepheline-syenites and anorthosites which are the most extensive and important occurrences of corundiferous igneous rocks at present known, whether they be regarded from a_petrological standpoint or as a souree of supply for the best quality of abrasive material. These rocks have been deseribed by Professor W. E. MillerS and others. The occurrences of corundiferous rocks in the United States has recently been reviewed by J. H. Pratt.|| The most noteworthy occurrences are those of Montana, * Experimentelle Untersuchungen iiber die Bildung der Minerale im Magma, Tschermak’s M.u.P.M. N.F. Band XVIII, [899. +Manual of the Geology of India, Economic Geology, Pt. 1, 1898. Memoirs, Geological Survey of India, Vol. XXX, Pt. 3, 1901. ft Op. cit. § Rpt. Bureau of Mines, Vol. VIII, 2nd pt., 1899, Toronto. || U.S.G.S. Bull. 180, 1901. Lawson. ] Plumasite, an Oligoclase-Corundum Rock. 22] where corundum is found as an original constituent of certain se >* lamprophyre dykes in Yogo Gulch described by Pirsson,* who refers its origin to endomorphism of the magma by absorption of the adjacent shales. A corundiferous mica-augite-andesite at Ruby Bar, Montana, is described by Kuntz,t and Pratt has noted a corundiferous augite-mica-syenite from the same or a neighboring locality, as well as a corundiferous biotite-syenite from Gallatin county, Montana.} The important occurrences of corundum associated with peridotites in the Appalachian belt described by Pratt appear to be concentration products on the contacts of the peridotite, and may therefore be secondary rather than pyrogenic, although Pratt regards them as differentiation produets of the same magma which gave rise to the peridotite. In addition to these occurrences it has been long known that corundum exists as an accessory in a variety of volcanic rocks, notably in the voleanie districts of the Rhine, but these have usually been looked upon as inclusions picked up by the magma and foreign to it. It seems probable, in view of the establish- ment of the pyrogenic origin of corundum in the cases above referred to, that many of these supposed exotic occurrences of that mineral will be recognized as products of the crystallization of magmas. The Discovery.—lIt is the purpose of the present paper to offer a contribution to this growing body of information regard- ing corundiferous igneous rocks. The writer first became aware of the existence of the rock which forms the subject of the paper by seeing a fragment of it in the lapidary shop of Mr. Kinrade of San Francisco. He secured the specimen, and on inquiry ascertained that it had been brought there by Mr. J. A. Edman of the Diadem Mine, Plumas Co., Cal. He thereupon communi- cated with Mr. Edman and subsequently visited him, and was by him conducted to the locality where the rock outerops. The credit of the discovery of this new and interesting rock, there- fore, belongs to Mr. Edman, although it is the writer’s privilege *U.S.G.S. 20th An. Rpt., Pt. III, p. 554 et seq. +Am. Jour. Sci., 4th Ser., Vol. IV, 1897, p. 418. ft Op. cit., pp. 30, 31. 222 University of California. [Von. 3. to call the attention of petrographers to its character and mode of oceurrence, in so far as these can at present be ascertained. The locality hes in a region of peculiar geological interest, occupying the northeast corner of the Bidwell Bar quadrangle as mapped by H. W. Turner of the U. 8S. Geological Survey. — It is on the lower flank of Spanish Peak about two miles due east of the summit, near the southwest margin of a broad belt of peridotite. It is thus near the line of faulting to which the bold eastern scarp of Spanish Peak owes its origin. The lower flanks of the mountain are traversed by numerous small ereeks which eut up the surface into a suecession of alter- nating ridges and gulehes. The corundiferous rock oeceurs on one of these minor ridges, and the corundum was first discovered by Mr. Edman as float in the adjoiing gulch, and by him traced to its source. The Peridotite Cut by Corundiferous Dyke.—The corundifer- ous rock at this locality oceurs in the form of a white feldspathic dyke cutting a rock which is referred to in several of Turner’s publications on the geology of the Sierra Nevada. In the 14th annual report of the U.S.G.S. he says; “The largest single dyke of serpentine which is known to have been originally a peridotite or pyroxenite occurs in the northern end of the range in Sierra and Plumas counties. . . . This serpentine dyke has a width, where it is crossed by the middle fork of the Feather River, of more than 3 miles.” In the 17th annual report he gives the following petrographical note concerning this rock: ‘Loeality: one and one-half miles west of Spanish Ranch post- office. Microscopically this is an apparently fine-grained purplish and green rock, evidently in part serpentine. Microscopically, the strueture is coarse granular, and the rock is largely olivine, in rather large anhedrons, intersected by a network of cracks, which cross at all angles, and along these cracks serpentine is forming. Fibrous serpentine and tremolite occur between the olivines evidently as alteration products. Associated chiefly with the serpentine are black streaks of magnetite in aggregates of minute grains. Chromite or picotite may be present but was not observed.” In a later publication* he modifies this deserip *The Bidwell Bar Folio, 1898. LAWSON. ] Plumasite, an Oligoclase-Corundum Rock. P23 tion as regards the tremolite by saying: “The colorless amphibole was at first supposed to be tremolite, which is a jime-magnesia amphibole. Chemical analyses and Microscopie examinations, however, show that there are two colorless amphiboles present, one monoclinic probably edenite, and the other orthorhombic probably gedrite.” The samples of rocks collected by the present writer at the place where the corundifer- ous dyke euts it agree fairly well with Turner’s description except as to minor details. Here the rock may be found both in a fairly fresh condition and also largely serpentized. The fresh rock has a well marked but rude schistosity. On fractures transverse to this schistosity it is of a dull greenish gray color and compact texture, relieved by long narrow blades of a light colored, cleavable mineral, and showing irregular partings in the plane of schistosity. On the cleavage surfaces the rock presents a silvery gray spangled appearance as a ground-mass, with numerous cleavage blades of the same light colored mate- rial. These blades le with their axes of elongation rudely parallel to the schistosity but in all orientations in that plane. They are about 51 mm. in size. Examined in thin section the rock is seen to be made up of but two primary minerals. The more abundant of the two agrees with olivine in its optical properties. It forms a mosaic of rather angular or occasionally subrounded anhedrons, which have an average size of .25 mm. Occasionally these show a tendency to elongation, so that one diameter may be twice the other, but for the most part they are approximately equidimen- sional in cross section. The olivine is not only a mosaic ageregate of anhedrons in this section, but many of these anhe- drons have a polyvsomatic structure. The anhedrons, whether simple or polysomatic, are traversed with irregular sharp cracks, and along these cracks incipient serpentinization may be observed as noted by Turner. Oceasionally this process has proceeded so far as to give rise to distinct patches of serpentine. Lying in this mosaic are elongated prisms of a colorless mineral having the optical characters of tremolite. This makes up about 20 per cent. of the rock. In the zone of the vertical axis it has idio- morphic boundaries, but the ends of the prisms are splintered 224 University of California. [Vor. 3. out. This is undoubtedly the mineral which Turner first identi- fied as tremolite and afterwards referred partly to edenite and partly to gedrite. It is a colorless monoclinie amphibole with extinction angles not exceeding 18°, showing the oblique emergence of an optic axis on (100). Turner does not give the chemical and optieal reactions which induced him to change his identification. The only other mineral present is magnetite, and this is secondary, being found only in shreds in the serpentine areas of the sections. Chemical Composition of Peridotite.—The rock when digested in a pulverized condition with strong acids fails to dissolve and yield gelatinous silica, and on this account a doubt arose as to the character of the mineral which on optical grounds had been determined as olivine. To resolve this doubt, and also to obtain information as to the chemical character of the colorless amphi- bole, the rock was chemically analyzed by Dr. W. C. Blasdale, to whom the writer desires to express his obligations. Dr. Blasdale’s analysis is as follows: SiO. 41.49 AlsO3 2,29 Fes Os 1.07 FeO Medel MeO 39.63 CaO 1.89 Loss on ig. 5.56 98.97 From this analysis the mineralogical composition of the rock has been computed to be as follows: Olivine 2(MgO,FeO) SiO» 44.97 per cent. Serpentine 2H2O,3Me0,2S8i02 Bole) 7 a2 Magnetite Fe.O;.FeO 139) ” xo: ( 2H.0,CaO,3Mg0, 48i0. 15.36 ” ” Edenite g = ) (MgO, A103, SiO» Ana? } 99.08 ” ” The analysis thus leaves no doubt of the peridotitic character of the rock notwithstanding its failure to yield gelatinous silica on digestion with acids. It reveals, moreover, the presence of an aluminous molecule which is supposed, in accordance with Turner’s observations, to be combined with the tremolite molecule aa0 LAWSON. | Plumasite, an Oligoclase-Corundum Rock. to form edenite. The degree of serpentinization is greater than would be inferred from an inspection of the thin slides. Original Edenite.—Turner regards the amphibole in the rock deseribed by him as secondary, but in the rock with which we are here concerned it appears to be as much an original mineral as the olivine. It is in part intergrown with the olivine in parallel intergrowth and its idiomorphie form, contrasting with the allotriomorphic character of the olivine abutting upon it, shows that for the most part it antedated in crystallization the latter mineral. It appears then clearly that the country rock in which the conundiferous dyke occurs is a peridotite and may for con- venlence be designated an amphibole-peridotite. In the more altered facies of this rock taken from the same locality and the same mass, serpentine is the predominating mineral and there are only residuals of the olivine and pseudo- morphs of the edenite. There is naturally much more secondary magnetite, and a notable amount of ealeite or dolomite in ragged patches occurs mixed with the serpentine. Extent of the Corundiferous Dyke.—The dyke of corundiferous rock whieh euts this amphibole-peridotite is of quite limited extent so far as the writer’s observation goes. The strike of the dyke is about N.N.W. or transverse to the axis of the ridge upon whieh it is found. There are but three exposures and these do not extend for more than 125 feet along the strike. The width of the dyke is about 15 feet, but its dip is difficult to determine, owing to the imperfection of the exposures. The slope is mantled with soil and with fragments arising from the disintegra- tion of the amphibole-peridotite and the exposures of the dyke project through this covering of loose material. The rock of the dyke is composed chiefly of feldspar and is white in color, being thus in marked contrast to the darker rock mass which it cuts. The Corundiferous Facies.—From a petrographical point of view the rock of the dyke is far from uniform. In the middle exposure, where a pit had been sunk by Mr. Edman at the time of the writer’s visit, it consists of a coarse allotriomorphie gran- ular aggregate of white feldspar in which are imbedded erystals of corundum. The feldspar is but shghtly decomposed and in thin section is seen to be finely striated due to twinning 226 University of California. [Von. 3. on the albite law. The symmetrical extinction angles of these albite lamellae do not exceed the low values characteristic of oligoclase. The specific gravity as determined on three selected fragments was found with the Westphal balance to be 2.630, 2.634 and 2.636, the average being 2.638. An analysis of the feldspar, which was kindly made by Mr. J. Newfield, of the Chemical Department of the University of California, gave the following results: SiO» 61.36 Al,O3 22.97 CaO 5.38 NavsO 8.08 H.O ie 99.51 This calculated to a water free basis gives the following molecular ratios: SiO» 1.045 Al, O3 .230 CaO 098 NasO 134 These ratios correspond to those of an oligoclase of the formula Ab; Ane with 2.7 per cent. of SiO» to spare. The Corundum.—The corundum is in crystals ranging in size from a few millimeters to over five centimeters in length. These are of a pale violet blue color. In most cases they are imperfectly formed but many were observed with well defined crystal forms, showing sharply hexagonal cross-sections. The faces of these erystals are rough and do not lend themselves to measurement with the reflecting goniometer. There is apparently but one habit represented and this is due to an acute rhombohedron without prismatic faces. The angle between two of these rhom- bohedra, measured over the basal edge with a contact goniometer, was found to be 164° and between the same two faces over the polar edge 120°. These values agree with those given for the form 6 (8.8.16.3). There is occasionally observed a parting im these crystals parallel to the base. The specific gravity of the corundum varies from 3.9 to 4.2 with an average value of about 4.0. LAWSON, ] Plumasite, an Oligoclase-Corundum Rock. 227 When the corundum erystals are broken off the fracture surfaces show not uncommonly sealy films of a lustrous silvery white, or pearly mineral of micaceous habit. The scales are brittle, and when examined on the stage of the microscope they have the characters of a biaxial mineral with small optic angele, rather low double refraction and negative character. They are, therefore, identified as margarite. There occurs through the feldspathie part of the rock a similarly appearing’ secondary mineral in the form of small veinlets and patches. In this case, however, the luster is more waxy and the color somewhat green- ish. The mineral is foliated, aud the seales when examined on the stage of the microscope show it to be unaxial and positive ‘and to have a feeble double refraction. Its speeifie gravity is 2.74. These data are insufficient for identification with any known mineral, but they agree most closely with the characters of a light colored chlorite. It appears to oeeur in the rock along minor breaks and dislocations. Chemical Composition of the Rock.—Representative hand speci- mens of the rock composed practically of only oligoclase and corundum were taken to determine the proportion in which these two minerals are present in the rock. The specific gravity of the rock was found from a series of four samples, weighing 165 to 442 erms., to be 2.789. Knowing this and the specifie gravity of both constituent minerals, as given above, the proportion was found to be oligoclase 83.64 per cent., corundum 16.36 per cent. Taking the round numbers 84 and 16 as the respective percent- ages of the two minerals. the bulk analysis of the rock is found to be as follows: SiO. 51.80 AlsO3 Binai9) CaO 4.54 Nav.O 6.82 HO 1.45 100.00 The Rock Type Defined.—It appears from the foregoing description that this interesting rock has resulted from the con- solidation of a magma having approximately the composition of oligoclase with an excess of alumina. This particular type of 228 University of California. (Vor. 3. rock magma does not appear to have been as yet recognized among the known. occurrences of rocks, and it is, therefore, proposed to name it, for convenience in reference, Plumasite, from Plumas county, in which it oceurs. For purposes of refer- ence to this type plumasite may be defined as a rock resulting from the consolidation of a magma having the composition of a medium acid plagioclase with an excess of alumina. The extent to which the alumina is in excess 1s not material to the defini- tion. It is characteristieally a coarse allotromorphie granular ageregate of acid plagioclase with idiomorphic crystals of corundum, but on its chilled margins may have a fine-grained porphyritie structure with phenocrysts of plagioclase in a plagio- ¢lase eroundmass. Other Facies of the Dyke.—At the exposure 100 feet northwest of that just deseribed the dyke has an exposed width of 15 feet. About two-thirds of the exposure on the southwest side consists of a very coarse-textured white feldspar rock the same as that above described, but without corundum so far as could be dis- covered. Seattered sporadically through this coarse feldspar rock there are occasional nests of a greenish gray mineral having a fibrous radial habit which proves on microscopic examination to have the characters of a colorless monoclinic amphibole. These are apparently secondary and not original products of the crystallization of the magma. The remaining third of the dyke on the northwest side is much finer grained and is porphyritie in structure, though apparently consisting wholly of white feldspar. It appears to be the chilled selvage of the dyke, but, owing to the unsatisfactory character of the outcrop, its relations to the coarse-grained portion of the dyke could not be determined. The only other exposure of the dyke is about 25 feet to the southeast of the first outerop described. Here the rock is again fine grained to microcrystalline and porphyritic. The porphyritie erystals range up to 5 millimeters in size, and usually show poly- synthetic twin striations on the cleavage faces. Optical reac- tions show that these porphyritic plagioclases are andesine. The groundmass in which these phenocrysts are involved is a very fine microgranitic aggregate of feldspar whose composition is Lawson. ] Plumasite, an Oligoclase-Corundum Rock. 229 undetermined. There is no corundum discoverable in this facies of the dyke. Correlation.—Turner has given us an account* of an extended series of white feldspathic dykes distributed throughout the gold belt of the Sierra Nevada, several of which occur in the vicinity of Meadow Valley to the east of Spanish Peak. These rocks are classed by Turner under the soda syvenites, and as the feldspar in those cases investigated by him consist almost wholly of albite, he ealls them albitites. The dyke with which we are concerned in this paper evidently belongs to this series, although even in the non-corundiferous facies it cannot be called an albitite. These dykes according to the writer’s observations vary considerably in their mineralogical composition, some being rich in quartz and others quite devoid of it, so that, although having a distinct consanguinity, they would fall into a number of petrographically different classes. Plumasite is the first of these in which corundum has been found, but others having this character will doubtless be found when the field is better known. * Notice of some Syenitic Rocks of California. Am. Geol., Vol. XVII, June, 1896, p. 375 et seq. University of California, April, 1903. $56.4 7% UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 9, pp. 231=236, PI. 20. ANDREW C. LAWSON, Editor PALACHEITE .- BY ARTHUR S. EAKLE 90058880nang, 2 0! . , Fa at OF 6 4 * Ny (} LH) io OF (3 25 Gi \\ : =Qy° Wy SI fe (Ay WIT Y < Pee, e, oe S eS a BERKELEY THE UNIVERSITY PRESS APRiL, 1903 PRICE 10 CENTS Za THE BULLETIN OF THE DEPARTMENT OF GEOLOGY OF THE UNIVERSITY OF CALI: FORNIA is issued at irregular intervals in the form of separate papers or memoirs, each | f embodying the results of research by some competent investigator in geological science. _ ty. me ¥ It is designed to have these made up into volumes of from 400 to 500 pages. The price aa per volume is placed at $3.50, including postage. The papers composing the volumes will be sent to subscribers in separate covers as soon as issued. The separate numbers may be purchased at the following prices from the University Librarian, J. C. Rowell, to whom remittances should be addressed:— © VOLUME 1. z No. 1. The Geology of Carmelo Bay, by Andrew C. Lawson, with Gieniea analy- ses and codperation in the field, by Juan de la C. Posada . Price; 25¢=e No. 2. The Soda-Rhyolite North of Berkeley, by Charles Palache ; | 2Pricéyroe No. 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome : Price, 4oc No. 4. The Post-Pliocene Diastrophism of the Coast of, Southern California, by . Andrew C. Lawson ' $ Price, 4oc — No. 5. The Lherzolite-Serpentine and Associated Rocks of the Potreo, San) tm one Francisco, by Charles Palache erie No. 6. Ona Rock, from the Vicinity of Berkeley, ‘containing a New Soda oe a Amphibole, by Charles Palache A Prigen06 No. 7. The Geology of Angel Island, by F. Leslie Ransome, ‘with a Note on the * Radiolarian Chert from Angel Island and from Buri-buri Ridge, San Mateo County, California, by George Jennings Hinde ; i REceeA se No. 8. The Geomorphogeny of the Coast of Northern California, by Andrew C. - Lawson . ‘ Price, 30c No. 9g. On Analcite Diabase from San Luis Obispo County, California, by | Harold W. Fairbanks ; pt Pricey ese No, ro. On Lawsonite, a New Rock- forming Mineral from the Tiburon Peninsula, Marin County, California, by F. Leslie Ransome . ; Price, 10e No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte . Price, 20c No. 12. On Malignite, a Family of Basic, Plutonic, Orthoclase Rocks, Rich in Alka- lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, by Andrew C. Lawson ; Price, 20c No. 13. Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene, near Berkeley, by John C. Merriam. 5 Price, roc No. 14. The Great Valley of seat a Criticism of the Theory of Isostasy, by F. Leslie Ransome . 4 m Price, 45c VOLUME. 2s : INfos iy ADoKS Geology of Point Sal, By Harold W. Fairbanks ee Price, 65c¢ No. 2. On Some Pliocene Ostracoda from near Beers by Frederick Chap- : man . Price, Ice No. 3. Note on Two Tertiary Faunas from the Rocks of the Southern Coast of Vancouver Island, by J.C. Merriam . sp eiice sia No. 4. The Distribution of the Neocene Sea-urchins of Middle California, and Its ’ Bearing on the Classification of the Neocene Formations, by John C. Merriam a 5 F Price, roc No. 5. The Geology of Point Reyes Peninsula, by F.M. Anderson. . Price, 25¢ No. 6. Some Aspects of Erosion in Relation to the Theory of the Peneplain, by wo S. Tangier Smith : Price, 20c No. 7. A Topographic Study of ‘the Islands of Southern California, by W. S. Tangier Smith : Price, 4oc No. 8. The Geology of the Central Portion of ‘the Isthmus of Panama, by Oscar H. Hershey. . a Price agen No. 9g. A Contribution to the Geology of the John Day Basin, by John C. Merriam Price, 35¢ ' No. 10. Mineralogical Notes, by Arthur S. Eakle . Bi pera seve se, Toc No. 11. Contributions to the Mineralogy of California, by Walter C. Blasdale Price, 15c” No. 12. The Berkeley Hills. A Detail of Coast Range Geology, by Andrew C. Law- : ~ son and Charles Palache ¢ F “ 5 a: z 5 . Price, 80c — UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 9, pp. 231=236, PI. 20 ANDREW C. LAWSON, Editor PALACHEITE BY ARTHUR S. EAKLE CONTENTS PAGE Introduction ee on aes EN OO Nee ag ore oes rte tee ce 231 Name of Mineral .... ..... Se ao NC rex Sree hE 9 ee eee eee Eee PBHl Oceurrence ....... ..... SE PR ceo CAS PE Sao e E ER Re PA 231 Crystallographic Characters .............2.0.:::00 sce 232 Measurements ee FN Se saieegt shee er ee ers ta 232 SS GO Mngen mn Clap EL AIO Mit eee cee ae teceen cect oe net eecnccee ores: ces ce teeuet lc dezeay cic rsetea sal A oecesducses-sa ete 232 Polar Hlements and Axial Ratio... 22... ...... .cceccecceececosec veeese seceseees osess scenes 232 PERO Te 1S ae rm eG alte as Beat weccceea cae, Stare ees casa see tosh picestee Aicesw, dey evel eba, seared Days} Waloullatede Mal) Cm. 8e ccs fo oekecceee Gece Sec tecMeacse, ntlvheve este sceaven! ; 236 Imibemtaciall PAM OOS gk ce cceslecceceraeedet cede cece cece teeecceeeces ate ee oun a oa oe LVN APUG LENO OSA IIS) eee yes Rg ere ee 234 (Georenalm@ Wanacters ese sano .s8 ccscess eeeeesseriqereeee ees ees cosasgeses SMe iawn ee epee OIC MIB CAT aGtens ern, cece tecasetterechavacteecssvecseeqteces Sees ote we eek Gran Call rO Clu eSa.te cesses rsecee ce en eee ease cesivecacseeaisrtesariecssssine tie ae. LOO HEBYMO STN OSUICS: ste es cs has sees sa hck scat vas osagas Riaandes. ct 228! Srv pease cs ol yeas eerie Nee 239 Composition ..... ........ Se ne Rte ete Met ocak aes caus ts gher eae: Stade castes inet ee 235 Jai)01] ON 1G) eee See Sa ert Der eee: SacI pte AM Ea 236 INTRODUCTION. Name of Mineral.—A mineral occurring in bright red erystals was found, about a year ago, in the Redington mercury mine, Knoxville, California, in considerable quantity. It proves to be a new hydrous basic sulphate of iron and magnesium, for which the author proposes the name palacheite, in honor of Dr. Charles Palache of Harvard University. Occurrence.—The specimens are loosely coherent aggregates of minute erystals, which readily crumble on the slightest pressure into smaller aggregates or bunches of crystals. There is no cementing matrix whatever, the specimens being merely inter- grown erystals; even the smallest crystal seems to be an 232 University of California. [Vou. 3. intergrowth, more or less parallel, of smaller individuals. The superintendent of the mine, Mr. J. B. Mason, who found the mineral and has kindly sent specimens to the writer, reports that the red sulphate was found by cross-cutting through an old stope which had been filled about forty vears ago, the mineral having formed in this stope with newly formed cinnabar and much sulphur. The heat developed from the decomposition of the mareasite was so intense where the mineral occurred, that the old timbers of the stope had become converted into solid charcoal. The specimens sent to the writer had much yellow sulphate asso- ciated with them, which is probably copiapite, although this has not yet been definitely proved. This mine is quite noted for the variety of sulphates formed from the decomposition of the sulphides, epsomite, knoxvillite and redingtonite,* and coquimbitet having previously been described from there. CRYSTALLOGRAPHIC CHARACTERS. Measurements.—The erystals were measured principally by the two-cirele method, although a few interfacial angles were also determined. The larger crystals, owing to their composite structure, give poor measurements, the prism faces being striated and often interrupted, and the bases wavy; but some of the smallest crystals, about 1 mm. in size, gave very exact readings, and these were chosen for the calculations. System and Habit.—The erystals are monoclinic and have but one habit, namely, short prisms terminated by the two basal planes. The prismatic zone and the base are in almost equal development, and the erystals in consequence resemble rhombo- hedvons. Polar Elements and Avial Ratio.—The average values of p’o, go and e’ determined from the coérdinates # and y’, for the prisms, clino-domes and bases, were as follows: p'o = 0.6852 ; qo = 0.3996 ; e = 0.5128. * Melville and Lindgren, U. 8. Geol. Sury. Bull. 61, 1890. +A. S. Eakle, Mineralogical Notes, Bull. Dept. Geol., Univ. Cal., Vol. 2, 315-326, 1901. EAKLE.] Palacheite. Do From these values the elements and axial ratio for the monoclinic erystals become 9° 51! po = 0.6097 ; go = 0.3556 5; e = 0. 4563 5 p= 162 a@:b:¢ = 0.6554 :1:0.3996 ; 8 = 117°9. Forms.—The forms oceurring on the crystals are as follows: ¢— 000i; b =0x = 3010} d = —20 = $2015 m= o = $110} a = 00= }100} »=—l, = 3111} 1 — 2 — 41201 n= 01 = 3011 § = —12 = }121} t = of = 3450} ) 0 == YO The base $001%, unit prism }110{ and clino-prism }120{ are the predominating forms. The prism faces are invariably vertically striated. The pinacoid }010{ is usually narrow, but always per- feet, without striations. The other forms occur rarely and are always very narrow, sometimes mere line faces, on the edges between the main forms. Figure 1, Pl. 20, shows the habit and usual combination; Fig. 2 shows, in addition to the main forms, some of the rarer ones, in their relative development. Fig. 3 is an orthographic projection of the forms on the basal plane. Calculated Table.—The following table gives the calculations for the eleven forms, arranged to correspond to Goldsehmidt’s Winkeltabellen: a = 0.6654 lg a = 9.816506 | lg a= 0.214881 temo = 9.785116 ay= 1.6411 po = 0.6097 c= = 0.8996 lee = 9. 601625 lg bo = 0.398375 Ig qo = 9.550962 bo = 2.5025 | go = 0.3556 Sie Helen lge =) mais we anes ea ee as 180 — BS P°® (f \ G25 “lg sin pS 9.949300 ge oat f 9.659271 lg 22 ae = 0.234154 h = 0.8898 | e = 0.4563 fp . | | a ’ | ® | 5 | (Prism) ; a plfie/2)/ ¢ | © |.4 |] m | | 2 Pn) » a\a|s | | | a ee pen ie ES es a | : ee a | | | 1 | © 0 |001 90° 00’ 27°09 272.09" 0° 00" 27° 09" 0° 000.5128 0 0.5128 2/b 0x%/010' 0 00.90 00 0 00.90 00 0 0090 00 0 aw ow 3 «0 | 100 90 a ‘90 00, 0 00:90 00,000 «~ 0 es 4|m| © |110|/59 45) “ | ‘* (90 00/59 45 |30 15 1.7147) & ce 511 nee 120|40 36) ‘* | ‘* | ‘* |40 36/49 23-/0.8573] ‘ 6 | t | m$|450\53 54] “| | ‘* |53 5436 05+1.3716) “ a 7 | ad |—20/201/90 00 40 37 40 37 0 00 40 37/ 0 00 0.8576 0 0.8576 8 | | 01/011|52 04/33 02 27 09/21 47/25 28/19 34: 0.5128 0.3996-/0.6501 9 | 0 | 02)021/32 41 43 31) “‘ |38 38/21 50/35 25| ‘‘ (0.7992 |0.9496 10 | p = T11/23 20 23 31| 9 47/21 47| 9 06/21 30 0.1724,0.3996 |0.4352 A es —P 721/12 10/39 16) ‘* |38.38| 7 40/38 13 ‘* (0.7992 0.8177 | | | | 934 University of California. [Vor. 3. Interfacial Angles.—The ealeulated, and some of the meas- ured, interfacial angles are as follows: Calculated, Measured. (110) : (110) 60° 80’ 60° 30’ (010) : (120) 40 36 40 36 (010) : (450) 53 54 53 52 (001) : (110) 60 47 60 40 (001) : (011) 19 34 19 3 (010) : (021) 54 35 53 40 (001) : (201) 68 06 67 45 (001) : (111) ASI) (eee (001) : (121) byl Xs; PHYSICAL PROPERTIES. General Characters.—The erystals are transparent and have a deep brick red color, vitreous luster and pale yellow streak. They are very brittle, have a hardness of 1.5 to 2, and a specific gravity of 2.075, determined with the Thoulet solution. Cleavage is very perfect parallel to the clino-pinacoid }010{ and distinet parallel to the unit prism }110;. Optical Characters.—The plane of the optic axis lies normal to the elino-pinacoid. The mineral is optically positive, and the acute bisectrix C makes an angle of about 12° with the vertical axis in the acute angle 6. Sections cut almost normal to the vertical axis show a good biaxial interference figure. The indices of refraction were determined approximately on thin sections by the Due de Chaulnes’ method, and gave for sodium heht a = 1.544 ; B = 1.548 5 y = 1.572. The double refraction from this would be high = .028. The optie angle caleulated from the indices gives Qing — 400 545 A measurement of the optic angle of a section mounted in Canada balsam, the latter having about the same index as P, gave: 2g — 405 The dispersion is p< v. The crystals are strongly pleochroic; €, deep orange red; Db, pale red; &, bright yellow. In thin sections the colors are much paler, b and & becoming almost colorless, while € becomes orange yellow. EAKLE. Palachette. 235 CHEMICAL PROPERTIES. Pyroqnostics.—The mineral strongly exfoliates, like stilbite, before the blowpipe, and is converted into an infusible brownish black, magnetic mass. Much water is given off in a closed tube, which does not react acid unless the heat is high enough to decompose the sulphate. It is difficultly soluble in cold water, but when the solution is heated it becomes decomposed with the separation of a bulky, yellowish red precipitate of ferrie hydrox- ide. The mineral is easily and completely soluble in dilute acids. It is perfectly tasteless. Composition.—The average of several analyses of the mineral gave for its composition Molecular Approx. Ratio. Ratio. Fes Os 19.51 122 1 MgO 9.35 .239 2 SO; Blea 480 4 - on Ke aie desu 19.03} 3908 1.793 15 HO above 100°C 12.75)" 99.51 The formula, therefore, is FeoO3.2Me0.4803;+15H2O0, and this requires the following percentages, which correspond very well with the analysis: Fes0; MgO SO; HO A fractional water determination was as follows: At 100°C 19.53 160 6.12 220 3.52 270 1.34 Above 280 Marl 32.28 All of the water could be driven off without decomposing the sulphate. About nine molecules were lost at 100° C, thirteen at about 270°, and the remaining two probably near 300° Twenty per cent. of the water driven off at 270° was reabsorbed over night by exposure to the air, and enough moisture was absorbed after several days to render the powder a pasty mass. 236 University of California. [Von. 3. RUBRITE. In the year 1890 Darapsky* published an analysis of an impure red sulphate, from Chili, which he named rubrite from its color, and later, in 1898,t he gave another analysis under the same name, although there is very little in common between the two analyses, and his derived formulas were quite different. This later analysis corresponds fairly well to that of palacheite, although he makes the formula for his mineral Fe203.2Me¢0.4SO03+18H20. From the size of his crystals it would seem as though something more than the mere chemical composition could have been deter- mined for his mineral. His deseription simply states that they were bright-red, long, orthorhombic or monoclinic erystals. In view of his meager deseription and the fact that palacheite bears no resemblance to the original material to which the name rubrite was given, the writer has no hesitancy in giving a name to the Knoxville sulphate. * Neues Jahrbuch, Min. 1890, 1, 65. t Ibid, 1898, 1, 163. University of California, April, 1903. BUELS DEPT. GEOL. UNIV. CAE. WA@IES s+) IAL 20); on UNIVERSITY. OF “CALIFORNIA PUBLICATIONS ; oi Bulletin of the Department of Geology 4 hyol, 3, No. 10, pp. 237-241, No. 11, pp. 243-248 - ANDREW C. LAWSON, Editor TA "4 ‘e . \ \ J ge) ; —s 4 h h th a ae | i , Ba At ! , me a ary ‘ ee i On TWO NEW SPECIES OF FOSSIL TURTLES Be he ae FROM OREGON Di Me ' the hy as jar ed ; tie ; BY 2 een Seay 35. 0. P. HAY , Bix NEW TORTOISE FROM THE AURIFEROUS GRAVELS OF CALIFORNIA Wartinn BY y ) W. J. SINCLAIR i\¥ fe } ni A { oy : eX \ ) iy on OF me a CX! | } x 4 ira < .< 7 .' ep, <*" ee, > Poveeeeeeoee! BERKELEY THE UNIVERSITY PRESS E. MAY, 10903 wee: PRICE 10 CENTS \ No. 3. Note on Two Tertiary Faunas from the Rocks of the Southern Coast of ‘ = THE BuLLwriN OF THE DEPARTMENT oF Gro1ocy OF THE UNIVERSITY OF ‘Gx FORNTIA is issued at irregular intervals in the form of separate papers or memoirs, eac ih} embodying the results of research by some competent investigator in geological science. It is designed to have these made up into volumes of from 400 to 500 pages. The price y per volume is placed at $3.50, including postage. The papers composing the volumes will be sent to subscribers in separate covers as soon as issued. The separate numbers s may be purchased at the following prices from the University Bee ap; Cc. Rowell, fom, whom remittances should be addressed: — : Bian So is, ihe ‘" ieee Na ; . VOLUME 1. RR ae No. 1, The Geology of Carmelo Bay, by Andrew C. 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On Analcite Diabase from San Luis Obispo County, California, by Harold) ae $ W. Fairbanks : IP 3 SE Price, 25c , AS No. i0. On Lawsonite, a New Rock- forming Mineral from the Tiburon Peninsula, > ae Marin County, California, by F. Leslie Ransome . & Pree Toce am cicth No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte - Price, Zocken te No. 12. On Malignite, a Family of Basic, Plutonic, Orthoclase Rocks, Rich in Alka- Bue. lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, fs. by Andrew C. Lawson. ce Price 200m hi No. 13. Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene, near : Be Re Berkeley, by John C. Merriam. “A Price, Loc oo” No. 14. The Great Valley of California, a Criticism of the Theory of Isostasy, by _ ‘em ; F. Leslie Ransome . > : Eris) ASC — a VOLUME 2 No. 1. The Geology of Point Sal, By Harold W. Fairbanks ; Paice? 65c No. 2. On Some Pliocene Ostracoda from near ia, by Frederick Chap- ; man . 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Law- te son and Charles Palache 5 F . . C : 5 Pace ws UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 10, pp. 237=241. ANDREW C. LAWSON, Editor TWO NEW SPECIES OF FOSSIL TURTLES FROM OREGON. BY ORs Haws, The testudinate remains here deseribed were collected by parties under the charge of Dr. John C. Merriam during the years 1899 and 1900, in the course of geological explorations in the John Day basin of Oregon. The materials are quite frag- mentary, and there is some question regarding the horizon from which some of them were derived. Nevertheless, it seems to the writer that the bones afford characters which will enable future investigators, obtaining haply better materials, to identify their finds. Of the remains sent me there are four lots, with numbers indicating localities where collected and their place in the record of the museum of the University of California, as follows: Museum No. 2219, locality No. 909, Rattlesnake beds, Rattle- snake Creek. Museum Nos. 2179, 2180, locality No. 815, Maseall or Rattle- snake beds, Rattlesnake Creek. Museum No. 552, locality No. 887, Maseall or Rattlesnake beds, Rattlesnake Creek. Museum No. 2192, locality No. 896, Maseall beds, Beaver Creek, near Crooked River. The lots about which there is doubt are those bearing the museum numbers 552, 2179, and 2180. The nature of the doubt is explained in the following extract from Dr. Merriam’s report on the geology of the John Day basin (Univ. Cal. Bull. Dept. of Geol., ii, p. 311, 1901): 238 University of California. [Von. 3. “The Rattlesnake gravels contain many vertebrate remains, most of which have hitherto been listed with the Maseall fauna. The Rattlesnake fossils, when weathered out, are frequently to be found resting upon the Maseall beds below, and as most of the material from both Rattlesnake and Maseall is found detached from the matrix, the difficulties in the way of separating the faunas are considerable.” The bones sent me are hard and thoroughly fossilized, and the color and the character of the fossilization appears to be identical in the two cases. For reasons given below I regard provisionally the questionable materials as having been derived from the Rattlesnake beds. According to Dr. Merriam’s report, the the Maseall beds belong to the upper Miocene, the Rattlesnake deposits to the Plocene. CLEMMYS HESPERIA sp. nov. I take as the type of this species the bone bearing the number 2219 of the Paleontological Department of the University of California. This is the left hyoplastron, having the outer posterior portion, which enters into the bridge, missing. Figure 1 repre- sents it the natural size and as viewed from below. The sutural edges are present which met the hyoplastron of the opposite side, the postero-lateral border of the entoplastron, the hinder extremity of the epiplastron, and the front of the hypoplastron. As will be observed, the humero - pectoral suleus, represented by a dotted band, crosses the entoplastron, while the pectoro-abdominal sulcus is well back on the hyoplastron. The structure FIGURE 1. of these parts is identical with that of the genus Clemmys, represented to-day on the Pacific Coast by Clenmys marmorata. The free border of the bone between the humeral buttress and the epi-hyo-plastral suture is acute. Hay.| Two New Species of Fossil Turtles from Oregon. 239 The bone thickens until it reaches a thickness of 7 mm. where the suture just named meets the entoplastron. At the inner posterior angle the bone is only 8 mm. thick. In lot No. 2179 there is a portion of a left hyoplastron which lacks the free border, but which in the portions represented is identical with the specimen above deseribed. I regard it, there- fore, as belonging to the same species and to the same formation. In this lot are ineluded also a portion of the right epiplastron (Fig. 2), the first right peripheral bone (Fig. 3), a right peri- pheral, apparently the eighth or ninth, and some other fragments. The epiplastron has the border which joined its fellow of the other side missing, so that it is impossible to determine accurately the width of the anterior lip of the plastron. However, this bone has been used in making the restoration of the front of the plas- tron, as seen in figure 1. Figure 2 shows this bone as seen from below. It resembles closely the same bone in C. guttata, except that its upper side was not so deeply excavated as in the latter species. According to the restoration the lip had a breadth of about 384 mm. SiN / “ FIGURE 2. FIGURE 3. The free borders of the epiplastron are subacute. Seen from the side, this border runs forward to the gulo-humeral sulcus and then turns rather abruptly downward, forward and inward. From the acute edge the bone thickens rapidly, until a thickness of 7mm. is attained. The gulo-humeral suleus has probably continued backward on,the entoplastron. A piece of the thickened border of the xiphiplastron of this specimen is present. It extends from the junction with the hyoplastron to just behind the femoro-anal sulcus. Most of the free edge is broken away, but enough remains to show that it was acute. It thickens gradually until, at the inner border of 240 University of California. (Von. 3. the surface above which was covered with horny skin, the thick- ness is 6mm. The femoro-anal suleus comes to the free edge 19 mm. behind the anterior end of the bone. Figure 3 presents a view of the first right peripheral both from above and from the right-hand edge, which joined the second peripheral. The left-hand border joined the nuchal. The first peripheral resembles closely that of C. guttata. It will be observed that the outer anterior angle of the first vertebral scute extends outward on the bone here described and comes into contact with the second marginal scute. We have the same arrangement here that we find in C. leprosa, as shown by figure 30, page 102, of Boulenger’s Catalogue of Chelonians. This indicates that the first vertebral seute was broader than it is in C. guttata. The peripheral mentioned above, probably the ninth of the right side, resembles somewhat that represented by figure 4; but it is shorter antero-posteriorly and higher, the fore and aft dimension being 15 mm., the height 19 mm. The jongitu- dinal suleus runs closer to the upper Pa a border than in figure 4. The figure \4 ra just referred to presents a view of the : | left ninth peripheral of an individual i : \ somewhat larger than the one just Z \ deseribed. It is part of a lot num- Figure 4. bered 552. Figure 4 shows the upper surface and the anterior end of the bone. Accompanying this bone there is the hinder outer angle of the hypoplastron, extending from the suture with the xiphiplastron "No. 11. Contributions to the Mineralogy of California, by Walter Cc dora No, 12. The Berkeley Hills. A Detail of Coast Range ‘Geology, by Andr ; Tti is designed to have these made up into volumes of from 400 to. 500 ‘pay es _Per. volume is placed at $3.50, including postage. The papers composing t ‘will be sent to subscribers in separate covers as soon as issued. The separat may be purchased at the following Prices ; from the Wet 5 ‘Librarian, - ee ' whom remittances should be addressed:— PONE sates) SOR: . The Post-Pliocene Diastrophism of the Goat of ase California, b . The Lherzolite-Serpentine and Associated Rocks of the Potred, ‘San . On a Rock, from the Vicinity of Berkeley, ‘containing a New Soda | . The Geology of Angel Island, by F. Leslie I Ransome, ‘with a Note onthe! i. f . The Geomorphogeny of the ‘Coast it Northern California, by Andrew (re. . On Analcite Diabase from San Luis Obispo County, California, by Herod . On Lawsonite, a New Rock- forming Mineral faba the Tiburon Peninsula, . Critical Periods in the History of the Earth, by Joseph Le Conte ay Price, 20c . On Malignite, a Family of Basic, Plutonic, Orthoclase Rocks, Rich in Alka- No. 14. by AndrewC. Lawson. > a Price Sigmogomphius Le Contei, a New Castoroid Rodent, from. the Pliocene, Dear ie Berkeley, by John C. Merriam. Sia “Price, Toe 4 The Great Valley of California, a Criticism of the Theory of Tee ee ‘ F. Leslie Ransome . . dey ‘Price, 45 i VOLUME, 2. Ee i * The Geology of Point Sal, By Harold W. Fairbanks ‘Price, | On Some Pliocene Ostracoda from near Berkeley, by Fredetick Chap- - Note ou Two Tertiary Faupas from the Rocks of the ‘Southern coast if . The Distribution of the Neocene Sea-urchins of ‘Middle California, and 14 i . The Geology of Point Reyes Peninsula, by F. M. Anderson Se . Some Aspects of Erosion in Relation to the Theory of the Peneplain, : A Topographic Study of ‘the Islands of Southern Calirocnial by 2 . The Geology of the Central P Portion of ‘the Isthmus of oes " No. 9. yng VOLUME 1. . The Geology, of Carmelo Bay, by Andrew C. Lawson, with ctemfel analy- ts ses and codperation in the field, by JuandelaC. Posada . apa 25c . The Soda-Rhyolite North of Berkeley , ‘by Charles Palache . . P The Eruptive Rocks of Point Bonita, by F. Leslie Ransome Andrew C; Lawson # Rs Price, Hee : Francisco, by Charles Palache Amphibole, by Charles Palache Radiolarian Chert from Angel Island and from Buri-buri Ridge, San Mateo County, California, by George Jennings Hinde . . Price, 4 Lawson Price, oe W. Fairbanks , Price, Marin County, California, by F¥ Leslie Ransome . ~ es Price ae : lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, man . Vancouver Island, by J.C. Merriam . Bearing on the Classification of the Neocene Formations, Py John . Merriam 3 BAN, a S. Tangier Smith Tangier Smith Hershey Mineralogical Notes) by Arthur S. Balle ‘son and Charles Palache as bathe ie ela Sane UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 12, pp. 249-263, PI. 21-24. ‘ ANDREW C. LAWSON, Editor NEW ICHTHYOSAURIA UPPER TRIASSIC OF CALIFORNIA. BY JoHN C. MERRIAM. CONTENTS. Introduction Ben ce eta n2 Rear eee see De ee .... 249 Relationships and systematic position 00000. ee ees 20 () Detailed description of new genera and species .......... ee ee 20D Leptocheirus, new genus ............ Leptocheirus zitteli 0... Vertebree and ribs... eee /Nal ev BMONe PTO] th pee eee es Anterior limbs ....... Sere ee 9 255 9 MROStertOr LMS) 2.cc-e-cseecccceeee es cceseaee-- a oy Oe RARE STIG Skull) eee Se et Joe gah a : ee ee ... 258 Wemti tions oa. -cs-cssecsc-cee geese = EAN OPE ate oie ele 259 Toretocmemus, NOW SeCDUS .W........... te... ees eee ee sense es eee ae 259 Toretoenemus ealifornieus ; Bee cc se eg en tee eS 260 WASHES og 23021 00 A ih 0 ee erp No a eee 260 JetaYSeVAKONe BHO bas BE ee ere ee ene ene 261 letorsyremacope Ibhawleyss ee ee ee ee ee Ne ee OG J Naiatyefenea Kop eh wal] of peers Ns ee aie Oe PERRY, ieee NOR nO a I ya oo 263 INTRODUCTION. In a large collection of Upper Triassic saurian material which has recently been presented to the University of California by Miss A. M. Alexander there are two Ichthyosaurian species differing considerably from any that have been described. Though we are as yet only partially acquainted with their structure, they seem to be generically distinct from all of the known forms. Both specimens were obtained from exposures of the Trachyceras horizon of the Hosselkus limestone oceurring a few miles northeast of Winthrop, Shasta County, California. 250 University of California. (Vou. 3. RELATIONSHIPS AND SYSTEMATIC POSITION. The Ichthyosauria previously deseribed from the Upper Triassic fauna of California comprise six species placed in the genus Shastasaurus. So far as the extremities are known, these species are characterized by extreme shortness of the limb elements. The humerus, radius and ulna are wider than long, while the phalanges are circular in outline and ordinarily with- out lateral notching. The coracoid is antero-posteriorly con- stricted or peduneulate, the ribs of the middle dorsal region have but one head, and excepting one form (S. perrini) the vertebral centra are distinguished by their shortness. Of the two new types, one (Pls. 21, 22 and 28) is character- ized by its elongated limb elements, tridactyle manus, notched or constricted phalanges, shield-shaped coracoid, and long verte- bral centra. For this form the new generic and specific name Leptocheirus zitteli is proposed. The second form (Pl. 24) has also the elongated type of vertebral centrum and the slender tridactyle limbs but differs from the other species, so far as known, in possessing dorsal ribs with widely forked heads. Its limbs differ from those of the other new type in that the posterior extremities are larger than the anterior instead of being much smaller. This form has been given the name Toretocnemus californicus. Both Leptocheirus and Toretocnemus are sharply separated from Shastasaurus by their limb structure. The slender pro- podial, epipodial, and phalangeal elements are wholly different from the greatly abbreviated forms known in Shastasaurus. From each other Leptocheirus and Toretocnemus are distinguished by the character of the rib articulation in the dorsal region and by the difference in the relative size of the limbs. Both of the new genera, as also Shastasaurus, differ consider- ably from the European Mixosaurus.* In that genus the limbs have elongated propodial and epipodial segments but are distinguished by being pentadactyle, by having four elements in the first row of the mesopodial segment, and by the articulation of two or *See E. Repossi. Il Mixosauro degli strati triasici di Besano in Lombardia. atti della soe. ital. di scien. natur. Vol. XLI, Fase. 3, p. 361-372, Tav. VII, IX, Nov., 1902. Merriam. ] New Ichthyosauria. 251 more distal ecarpals on the intermedium. The arches, vertebrae, and dentition are also, as far as known, different from the corresponding structures in the Californian forms. From Ichthyosaurus the new genera differ in the form of their pectoral and pelvic arches, the elongation of their epipodial segments, and the constant notching with frequent double notehing or shafting of their phalanges. Including the forms here described, six distinetly separated groups of Iechthyosaurians designated as genera are now known. These groups may be characterized as follows: Mixosaurus. Dorsal ribs mainly single-headed. Coracoid peduneulate or with anterior and posterior emargination. ‘Seapula, ischium, and pubis much expanded distally. Inter- clavicle triangular, with concave borders. Limbs pentadactyle, propodial and epipodial segments elongated. Elements of epipo- dial segments separated by a wide cleft. Phalanges notched, sometimes with double notching or shafting. Four elements in the proximal row of mesopodial region. Intermedium supporting at least two elements distally. Dentition differentiated. Leptocheirus. Dorsal ribs, so far as known, single-headed. Coracoid elliptical, without emargination; seapula expanded distally; clavicle broad; interclavicle probably broadly triangular. Limbs tridactyle with a very rudimentary fourth digit. Pro- podial and epipodial segments elongated. Elements of epipodial segments separated by a wide cleft. Phalanges notched on one or both sides. Three bones in the proximal row of mesopodial segments. Carpus and tarsus with linear arrangement, the intermedium supporting a single element distally. Shastasaurus. Ribs of dorsal region mainly single-headed. Jaudal hypocentra uniting to form long chevron bones. Coracoid peduneulate; scapula, ischium, and pubis much expanded distally. Pubis with deep obturator notch. Elements of pro- and epipodial segments greatly shortened. Radius and ulna separated by a cleft. Ulna considerably smaller than radius. Oymbospondylus (2?) As yet, too imperfectly known for satisfactory generic description. Toretocnemus. Ribs of the middle or posterior dorsal region with widely forking heads. Caudal hypocentra uniting to form 252 University of California. [Von. 3. cheveron bones. Ischium and pubis much expanded distally. Pubis with obturator foramen. Limbs tridaetyle with rudi- mentary fourth digit, structure in general as in Leptocheirus. Posterior limbs larger than anterior. Ichthyosaurus. Ribs of dorsal region double-headed except- ing a few of the most posterior. Coracoid generally pedunculate or with emargination. Seapula, ischium, and pubis narrow. Bones of the epipodial segments greatly shortened, generally in contact along their inner borders. Notching present on only a few phalanges on the anterior border of limb. Number of digits varying from three with a rudimentary fourth to ten. Dentition isodont. Baptanodon, Opthalmosaurus. Propodial elements articulat- ing distally with three greatly shortened epipodial bones. Dentition considerably reduced. The subdivision of the order Ichthyosauria into families was attempted by Baur,* who set up a family for each of the genera known at that time, viz., Mixosauride, Ichthyosauride, and Baptanodontide. To these three the writer has suggested the addition of the Shastasauridet as a group sharply distinguished from the others. Repossi’s recent paper shows Mixosaurus to be much more like Shastasaurus than was indicated by previous descriptions. The two genera are, however, distinctly separated, the types of limbs particularly being widely different. Of the two new genera here described Leptocheirus is nearer to Mixo- saurus than to any other of the genera but has throughout a different type of extremity and pectoral arch, while the dentition shows no signs of differentiation. Toretocnemus is like Lepto- cheirus in its type of limb, like Shastasaurus in the form of its pelvie areh and chevrons, and like Ichthyosaurus in the forking of its dorsal ribs. The question as to how the genera in the order Ichthyosauria should be grouped was one which did not seem difficult to solve when only Ichthyosaurus, Baptanodon, and Shastasaurus were fairly well known and but a small part of the skeleton of Mizo- saurus had been described. Now that Mixosaurus has been *G. Baur, Ueber den Ursprung der Extremitaten der Ichthyopterygia, Ber. d. XX Versam. d. Oberhein. Geol. Ver. Vol. XX, p. 3. * Bull. Dept. Geol. Univ. Calif., Vol. 3, p. 87. Merriam. | New Ichthyosauria. 25% carefully described and additional forms have been obtained from the Triassic of California, it becomes a much more difficult matter. To settle it satisfactorily involves a discussion of the primitive characters and the course of evolution of the Iehthyo- sauria. This is deferred to a study of the subject to appear in a later paper. DETAILED DESCRIPTION OF NEW GENERA AND SPECIES. Leptocheirus. New Genus. Caudal vertebra elongated. Dorsal ribs single-headed. Coracoid shield-shaped, much elongated antero-posteriorly, without anterior or posterior emargination. Extremities with ‘three slender digits and rudiment of a fourth. Anterior limb much larger than posterior. Elements of the propodial and epi- podial segments of anterior and posterior limbs much longer than broad. Epipodial bones separated by a wide cleft. Bones of first and third rows of the mesopopial, metapodial, and phalangeal regions all notched on one or both sides. Carpus and tarsus with linear arrangement, three elements each in the in the prox- imal and distal rows, intermedium articulating distally with but a single bone. Dentition isodont, conical teeth set in open grooves. Leptocheirus zitteli n. sp. Pus. 21, 22, AND 23. The type specimen (No. M 8099, University of California Paleontological Museum) is represented by the lower half of a skull with a part of the dentition, the complete pectoral girdle, both anterior limbs, and numerous fragmentary ribs, vertebrae, and abdominal ribs. It was discovered by Miss A. M. Alexander in the Trachyeeras zone of the upper Triassic limestones at the Cove near Madison’s Ranch on Squaw Creek, Shasta Co. Vertebre and ribs.—The only well-preserved vertebra present is an anterior caudal (Pl. 23. fig. 4) with the following dimen- sions: length 14 mm., height 22 mm., greatest width 24 mm. The end faces are very deeply coneave, sloping sharply from the periphery and almost meeting in the center. The diapophyses are small but have considerable lateral projection. The articular surfaces for the reception of the lower arches are situated on 254 University of California. LVon. 3. rather prominent apophyses. The centrum is hexagonal in cross-section, the inferior surface and the lateral areas above and below the diapophyses being flat or shghtly concave. The ribs are very imperfectly preserved and only one speci- men was found in which the form of the head and shaft can be seen distinetly. The single head is twisted backward and both sides of the shaft are grooved, the posterior more deeply than the anterior. The form of this rib is similar to that in the dorsal region of Shastasaurus perrinit. A great many of the abdominal ribs are present in their original positions. They are in five linear series like those of Ichthyosaurus. Anterior arch.—Excepting the clavicles and the inter-clavicle, which had slipped forward a short distance, the bones of the pectoral girdle were all in their natural positions, with the hmbs in place on each side. The coracoids (Pl. 21, fig. 2) are very much expanded antero-posteriorly. Their diameter measured in this direction is twice the length of that taken transversely. Their form is roughly elliptical. The anterior and posterior ends are gently-rounded and there is no trace of an anterior or posterior emargination. There is no pedunculation of the portion artic- ulating with the humerus and seapula as in Shastasaurus and Mixosaurus, though the proximal portion is considerably thick- ened. The portion next the median line is considerably thickened by a high ridge running obliquely forward. The scapulw (Pl. 21, fig. 2) are short and broad, having the general form seen in Shastasaurus. The articular surface is curved so as to form two fairly distinct facets for the coracoid and humerus. The anterior hook is shorter and the notch below it not so well marked as in Shastasaurus osmonti ov alexandre. As the posterior angle of the upper margin is very thin, it probably did not extend far beyond the limits given in the figure and was therefore shorter than in S. osmontt. The clavicles (Pl. 21, fig. 1) are represented by two heavy, broad bars meeting, or possibly overlapping, on the median line in front of the coracoids. The ends next the scapule are broken away so that the total length of these elements can not be determined. The ends next the median line are considerably broadened and are concave on the posterior side. As far as can MERRIAM. | New Ichthyosauria. 255 be determined the clavicles are much like those of Shastasaurus alexandra and osmonti. An elongated, triangular bar, shaped somewhat like a boom- erang, stretches across the median line below the contact of the clavicles and possibly represents the interclavicle (Pl. 21, fig. 1, Ie and Ie’). One-half of the triangle is perfectly preserved. The angle on the other side has been broken away, but had probably a form similar to the part present. The obtuse angle on the convex side of the bone may represent the median stem of the interelavicle in Ichthyosaurus. If this element is entire the posterior angle or median stem is much more reduced than in any other known Ichthvosaurian. MEASUREMENTS. Coracoid Antero-posterior diameter .. 0.2.2... ceeeeeeeeee eeeeeee eee 72 mm. MUTANS VETS OxCLe i) CU OYen see ee nee ea senes cence pence arene tens Beez 35 Greatest thickness at proximal end... 0.0 oe. 12.5 Greatest thickness on distal margin... 15 Seapula Thorn Gaon os neon aes esscseeeszcacs Bee ate Peers 40 Thickness at proximal end ....00.2.. eet ceeeeeeeeeeeeee cote 1 Width at proximal Gm oon. cece, ececece ce sce sence eeeeeeee enon *19 Claviele Width at end next median line... 00.0. ee 16 Width in middle of shaft —...... ee eee ere Nee aie 11 Anterior limbs (Pl. 22, fig. 1).—In agreement with the gen- erally elongated type of the limb, the humerus is considerably longer than broad. The distal end is wider than the proximal, having a transverse diameter equalling two-thirds the length of the bone. The trend of the anterior border is nearly at right angles to that of the distal margin, while the posterior border slopes backward. This means that the posterior side of the limb would receive a little less power than the anterior side, a fact that might have some influence in determining the location of reduction in the phalangial portion of the limb. In the middle of the anterior margin is a sharply eut noteh which is opposite the deepest part of a much broader indentation of the posterior side. This constriction of the middle of the humerus clearly represents the original shaft of the bone. Its presence here *A pproximate. 256 University of California. (Vou. 3. helps to explain the occurrence of a similar constriction in the more specialized humerus of Shastasaurus. A prominent ridge on the upper side of the proximal end is opposite a much larger elevation corresponding to the pectoral ridge on the inferior side. Both prominences extend to about the middle length of the humerus. A narrow ridge on the posterior distal angle of the upper side is opposite a similar elevation on the ulna. The radial and ulnar borders are both sharply coneave as in Ichthyo- SAUPUS. The radius has exactly one-half the length of the humerus. The anterior border is nearly straight, showing only a faint indentation near the middle. The posterior border is deeply coneave. The surface of contact with the radiale takes up nearly the whole of the distal end. The contact with the intermedium is only along the posterior angle. The ulna has a deeply coneave anterior border, and as in Mizxosaurus shows no emargination on the posterior side. The facets for the intermedium and the ulnare are of nearly the same length. ue lg Z-— Weare SZ VE_=—Z a Sie —<—e Ay Zz \ \ \\ \ VAX Vi SS Nes Ss: Wy g Y | EXPLANATION OF PLATE 22. Leptocheirus zitteli n. gen. and sp. Figures reproduced natural size from the type specimen. Fig. 1.—Superior side of left anterior limb. 1, radius. Fig. 2.—Posterior limb. f¢, tibia. BULL, DEPT, GEOL, UNIV. CAL. VO©lor3)-Rlee 22; Hs) Lf suf ly, AA s EEN TAT tt cea} a cot WALES v KEK SAN NIA K Ne f 1? \ {ied i Miah, ee ean eae ima 3 mi f pe Rb ary tint Zep \ Se Fig. EXPLANATION OF PLATE 23. Leptocheirus zitteli n. gen. and sp. Figures reproduced natural size from the type specimen. g. 1.—Right side of skull. g. 2.—Cross-section of posterior portion of the lower jaw, taken above the point marked A on the lateral view of the skull. g. 3.—Cross-section of the upper and lower jaws, taken at the break immediately behind the point marked Sp on the lateral view of the skull. 4,.—Lateral view of an anterior caudal centrum. L, lachrymal. Mx, maxillary. J, jugal. Po, postorbital. LEGEND FOR FIGuREs 1 Se, sclerotic ring. D, dentary. Sp, spenial. x Sa, supra-angular,. 9 b=) AND 3. angular. , articular. doubtful element. cross-section of tooth. BULL. DEPT. GEOL. UNIV. CAL. VOL. 3, PL. 23. EXPLANATION OF PLATE 24. Toretocnemus californicus n. gen. and sp. Figures reproduced natural size from the type specimen. Fig. 1.—Inferior side of right posterior limb. 17, tibia. Fig. 2.—Right anterior limb. 1, radius. Fig. 3.—Pelvie arch. Fig. 4.—Middle dorsal vertebre and a rib from the same region. oe BULL. DEPT. GEOL, UNIV. CAL. VO Ets haan eee GaN nel SALIF IA PUBLICATIONS tin of the Department of Geology _ 65-275, Pls. 25-27. _ ANDREW C. LAWSON, Editor 5 Ww ‘ . MENE- wey ‘SAN DIEGO CO., CALIFORNIA , “BY 13: "WALDEMAR T. SCHALLER ¥ ye Wy, SATZED Perse er eeves see" A } \ BERKELEY THE UNIVERSITY PRESS | | SEPTEMBER, 1903 Ai PRICE 10 CENTS 7 oe may be purchased at the following prices from the University Librarian, i ros Rowe whom remittances should be addressed: — ; No. I INO; 42 No. 3 No. 4 No. 5 No. 6. No. 7 No. 8 No. 9 No. 10 No. II No. 12 No. 13. No. 14. No. I No. 2 pUNo: 3 No. 4 No. 5 No. 6 No. 7 No. 8 No. 9. No. Io. No. It. Contributions to the Mineralogy of California, by Walter (es eee No. 12. It is act ace to have these made up into olunied of from 400 ‘to 500 pages. te per volume is placed at $3. 5°, including postage. The papers composing they . The Geology of Carmelo Bay, by Andrew C. Lawson, with chemical ‘obi . The Soda-Rhyolite North of Berkeley, by Charles Palache ., be) PERL Commo . The Eruptive Rocks of Point Bonita, by F. Leslie Ransome bem rnole, 405 . The Post-Pliocene Diastrophism of the Coast of Southern California, by . The Lherzolite-Serpentine and Associated Rocks of the Potreo, San) ty wae *: Francisco, by Charles Palache eaten ; . On a Rock;'from the Vicinity of Berkeley, ‘containing a New Soda Price, 30c . The Geology of Angel Island, by F. Leslie Ransome, ‘ait a Note on the ae . The Geomorphogeny of the Coast of Northern California, by Andrew C. ~ . On Analcite Diabase from San Luis Obispo County, California, by Harold . On Lawsonite, a New Rock- forming Mineral from the Tiburon Peninsula, ‘ . Critical Periods in the History of the Earth, by Joseph Le Conte . _ Price, 20c . "On Malignite, a Family of Basic, Plutonic, ‘Orthoclase Rocks, Rich in Alka- Lhe Geology of Point Sal, By Harold W. Fairbanks . Note on Two Terteny, Faunas from the Rocks ‘of the Southern che . The Distribution of the Neocene Sea-urchins of Middle te and | . The Geology of Point. Reyes Peninsula, by F, M. Anderson ats . Some Aspects of Erosion in Relation to the Theory of the Peneplain, by W. . A Topographic Study of the Islands of Southern California, by . The Geology of the Central P Portion of the Isthmus of Panama; Py, Oscar ie Ds VOLUME 1, 7 te ses and’ codperation in the field, by Juan de la C. Posada 5 Price, 25¢° oe Andrew C. Lawson ; . Price, os # Amphibole, by Charles Palache ~ Radiolarian Chert from Angel Island and from Buri-buri Ridge, San Mateo County, California, by George Jennings Hinde. . _ Price, 45c¢ Lawson i _ Price, wel mt W. Fairbanks 5 Price, 25¢ S Marin County, California, by F. Leslie Ransome . 4/2 # Price, toc” lies and Lime, Intrusive in the Coutchiching Schists of Poohhah Lake, de Tea by Andrew C. Lawson 2 Prices, 20c/ seem Sigmogomphius Le Contei, a New Castoroid Rodent, ‘iden the Pliocene, near Berkeley, by John C. Merriam. : f . Price, roc | The Great Valley of California, a Criticism of the Theory of Isostasy, by he F, Leslie Ransome . 3) eas a - = eee 45¢ VOLUME 2. . On Some Pliocene Ostracoda from near Berkeley, by Frederick | Chap- bit man Vancouver Island, by J.C. Merriam ~ Siaegale.e Bearing on the. Classification of the Neocene Formations, b oy Merriam Q i ae S. Tangier Smith ; ae Tangier Smith : Hershey : A Contribution to the Geology of the John Day Basin, by Jobn Ci / Mineralogical Notes, by Arthur S. Eakle “ais f The Berkeley Hills. A Detail of Coast Range Geology, By: aaae son and Charles Palache - Sys Bhat ne UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 13, pp. 265=275, Pls. 25=27. ANDREW C. LAWSON, Editor SPODUMENE SAN DIEGO CO., CALIFORNIA BY WALDEMAR T. SCHALLER CONTENTS PAGE (@ CCUNTE TIC Geer co ee eet sass eee geen ia gots Sere eases nee DO ReCE:, Dante, eee 265 TU OC ANTS Sere cee notes oa dels geet ce Ef i ONT ROE NR ne ee 265 Mode of Occurrence : 266 Deseription of Crystals 267 BEE CTS 116 Saeco ee ay Pe een EET ca anietate cee Pace oc ; 267 TEU ODE rie eee tretenese eae PT ON oe ce se a ae, OR aac see eee ai soe _ 269 JDRolal, Ake bese eee eee NE ee art a MR Sa NS ree es On‘ the Unit Prism ...................... pele eee one ee eee Pa eee On the Clinopinacoid Physical Properties ............... General Properties Optical Properties............. ee oem te ee Ns ee RE LPP ay ee eee os 273 (Clayewaomiorsy Ckavreaty oYoXspt iy op ote cies eee eee eee he ese ree eee nS 274 OCCURRENCE. Localities. —Beautiful transparent spodumene of deep am- ethystine purple, rose and magenta colors, has so far been found in two localities in southern California. The one from which most specimens have been obtained is situated about two miles north of Pala, San Diego Co., and this locality was visited by the writer during the past summer. The other place of occurrence is somewhere in the San Jacinto mountains, probably not far from Cuahuilla, Riverside Co., which is about twenty- five miles from Pala. It is probable that with further explora- tion other localities will be found in the Smith mountains, San Diego Co. and also in the San Jacinto mountains, Riverside Co. Ss agoman lnstify tin 24 1908 ao 266 University of California. (Vou. 3. Mode of Occurrence.—The formation in which these fine crystals are found at the Pala locality consists of a pegmatite dike, dipping westerly at a low angle, perhaps 20° It is more or less broken, and, as a whole, seems to form the surface of much of the slope of the hill, on which it oceurs. The dike is rather broad, but irregular in its present shape, and has a thickness of probably not more than thirty feet. Plate 25 is a photograph of the locality, looking north-west. So far as the mining developments have shown, only a small portion of the dike is rich in lithia minerals. Ordinarily, the dike is a coarse muscovite granite, the orthoclase and quartz predominating, containing many rounded prisms of black tourma- line, with broken ends. Lepidolite occasionally seems to replace the muscovite and when it does, red, blue and green tourmalines replace the black variety. It is with these gem tourmalines that the spodumene occurs. While the tourmaline and lepidolite are frequently inelosed in the quartz and feldspar, no such inclusions of spodumene have been found. The latter mineral always occurs associated with the other minerals, but never penetrating them or penetrated by them. It occurs in pockets and these facts seem to indicate that the formation of the spodumene is later and not coincident, in time of formation, with the tourma- lines and with the dike. The dike cuts across the large intrusion of dark rock occuring at Pala and briefly mentioned by Dr. H. W. Fairbanks* This large body of dark rock, several miles across is surrounded on all sides by granite. It is in this same body of rock and hardly a mile from the spodumene locality that the well known lepidolte mine is situated from which so many specimens of the fine-grained white lepidolite with the radiating groups of rubellite have been obtained. This large body of lepidolite occurs in a similar pegmatite, having the same general strike and dip as the dike carrying the spodumene, which mineral has not as yet been found in the lepidolite mine. The dark rock forming the footwall of the dike in which the spodumene occurs, is a diorite, consisting of hornblende, a plagio- elase, and (subordinate) orthoclase with accessory magnetite and apatite. * Ninth Report State Mineralogist (California. ) SCHALLER. ] Spodumene from San Diego County. 267 The hornblende is common green hornblende, with usually ragged outline, and possesses normal optical properties. b=—b,eAc = 16°. The pleochroism is & = light yellow to light olive green, b — dark olive green, C = sea green to blue ereen. The absorbtion is C > ba. The triclinie feldspar predominates as is shown by the albite twinning lamellae present. Symmetrical extinction angles gave values from 30° to 85°, making this feldspar labradorite. The orthoclase occurs sparingly in nearly square sections and is distinguished from the labradorite by its lower relief and birefringence. From its structure and mineral contents the rock is evidently ‘a basiediorite containing some orthoclase. From a deseription of the other locality, the mode of oceur- rence of the spodumene there, seems to be similar to that at Pala, being a dike in “blue granite” (the name locally given to the diorite). DESCRIPTION OF CRYSTALS Forms.—Only the prismatie zone is well defined on the specimens seen by the writer; both ends of the crystals are rounded off, and any forms occuring there are practically unde- terminable. On one of the smaller erystals, the two forms s = $121} and p = {112} may possibly be present.* The Dana Gat. Pa = -(G+1)2 —2(p+1).2q = pq measurement of these two forms, with the two circle goniometer, eave the following results: Measured. Calculated. $ p p p S11) itty 37° 14’ fomeo! 38° 46 72° 56’ p= —4 = {112} 21 05 Bul Gy 20. 05 34 04 The forms in the prism zone, however, can easily be determined. They are b= 00 = §010} n= 03 = }130} & = 00 — 3100; A= 0} = $350} N= a — NO 1 = $0 = $3205 * The orientation of the crystals in this paper corresponds to the one given in Goldschmidt’s Winkeltabellen. To change the indices to those given in Dana’s System, the following transformation symbols (Gdt. Index 3) are used. 268 University of California. [Vor. 3. The measurement of the angles of these forms with those ealeulated, are given in the following table. Measured. Calculated. $ p p p b= 00 = $010" 0° 06" 90° 00" 0° 00' 90° 00" a = 00 = }100} 90 00 e 90 00 oN M= © }110{ = 43: 330 s 43 30 = N= 03 = 41304 17 06 % 17 33 ‘* A= 0§ = $350} 29 50 29 39 i L = $0 3320} 55 OL e 54 54 ‘i The form A = ©} — }350{ is new for spodumene and occurs but once, as a small face. The form n = ©3 = }130{ was measured by means of a wax lmpression, as the erystal on which it occurs is too large for measurement with the reflection goniometer. The unit prism is always present, and measurements of ten faces gave the following values: ¢ angle on m = © = $110} 43° 30° 43 31 43 29 43 28 43 36 3 26 43 24 3 33 43 383 3 30 Av. = 48° 30’ This value agrees with the one given by Dana in his System, but varies somewhat from the angle obtained by Brush and Dana* on cleavage faces of the Branchville, Conn., spodumene, their results giving 43° 36.5% The interfacial angles on the large crystals were measured with a hand goniometer and the averages of these measurements are shown in the following table. Measured. Caleulated. (110) : (110) 93° 18’ 93° 00/ (110) : (110) 87 24 87 00 (110) : (O10) 44 00 43 30 (110) : (100) 46 36 46 30 (100) : (010) 89 30 90 00 The unit prism, while always present is not always equally developed in its four faces, two parallel faces being frequently * Amer, Journ. Science, 1880 (3), 20, 257. ScHALLER. | Spodumene from San Diego County. 269 much larger than the other two. The erystal thus presents a tabular appearance. The orthopinacoid is rather frequently present, though oceasionally it is very narrow and rounded to such an extent as to render it difficult to definitely decide if it be present or not. Then again, it may be very broad makine the crystal tabular. A marked feature of the orthopinacoid is that it is always deeply furrowed vertically. The clinopinacoid is not of frequent occurrence, though it has been noted a number of times, from a narrow face, less than a millimeter wide to one almost a centimeter in width. Fig. 2, Plate 26, shows the erystal having the broadest clinopinacoid. From left to right the faeces in the prism zone, on this erystal, are (130) (very narrow), (O10), (110), (100) (furrowed). The orthopinacoidal faces are the only ones striated. Habit.—Three habits are noticed in these erystals, depending on the relative size of the faces in the prismatic zone. The most common habit and the one that is more or less confined to the smaller erystals, is a tabular form resulting from the inequality in size of the prism faces. Other faces, such as the pinacoids are usually absent from erystals of this type. The second most frequent type is where the orthopinacoid is very large and the erystals become tabular parallel to this form. This habit seems to be restricted to the larger erystals. In the third habit, all three forms, the prism and the two pinacoids are equally developed and the erystal becomes octago- nal in shape. This habit is of rare occurence. Plate 26 is a photograph of seven erystals. Crystal 6 has the first habit, erystals 4 and 7 have the second habit, and erystal 2 has the third habit. ETCH FIGURES. On the Unit Prism.—A very marked feature: of these erystals is the profusion of natural eteh figures which thickly crowd all of the natural faces of the crystals, except the orthopinacoid. Even cleavage (prismatic) pieces frequently show them. On the faces of the unit prism they are especially thiek as can be seen in Fig. 6, Plate 26, which is a crystal tabular to a prism 270 University of California. [Vou. 3. face. The etch figures are usually triangular in shape and vary in size from a maximum leneth of about three millimeters and width of one millimeter to ones of miscroscopie size. Not infre- quently there will be several smaller ones in the base of a larger one. Occasionally a long string of the figures will run across a prism face, in an approximately horizontal direction. The orientation of these triangular pits with reference to the crystallographic directions, varies somewhat but, in general, is fairly constant and is shown in Fig. 1. The position of these Fig. 1. Showing position of Fig. 2. Showing position of etch figures on unit prism face etch figures on the four unit CU On: prism faces. figures on the four prism faces is shown in Fig. 2. It is noticed that they always point away from the orthopinacoid and the angle nearly 90° is nearest the clinopinacoid. Rarely the triangle passes into a trapezium by the addition of a fourth side, as is shown in the middle figure of Fig. 1; very few of the edges are perfectly straight, being move or less rounded, but they are mostly all drawn straight. Fig. 1, Plate 27, shows a photomicrograph of the common appearance of these etch figures —a large number of imperfect ones Closely crowded together. Fig. 2 shows a view of the best group of etch figures that could be found on any of the erystals. SCHALLER. ] Spodumene from San Diego County. 271 It represents the face (110) while the one to the left of it repre- sents the face (110). A detailed study of these etch figures shows that they consist of four faces: three side faces and a base. Fig. 1 gives in detail a view of one of these pits. The bottom or the face lettered m is parallel to the unit prism. The face x corresponds to the prism {320}, the face y to {8.14.3} or $351}, and the face z to $11.10.3'. The measurements on which these determina- tions are based, are as follows: Measured. Caleulated. p p p p i ose 110 43° 24’ 90° 00’ 43° 30! 90° 00’ i oo ==. 1850+ 55 49 mt 54 54 as D5 40 D6 09 COKHN MIO yayeanays} i lao 34 33 81 44 34 20 82 04 34 44 82 19 32 38 82 04 y | av. 83° 57 82 02 == bij = Shik f te iS 35 O01 82 39 g =—1f 42={17.10.3} 40 44 80 20 40 15 79 47 40 29 79 25 41 06 80 06 40 23 79 22 av. 40 41 79 48 For the face y the measurements are approximate for the two symbols }8.14.3{ and }351{ and the simpler one may there- fore be chosen. Quite frequently the faces m and # gerade insensibly into one another or the face m may be entirely lacking. gPricetoces = No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte. Price, 0c _ No. 12. On Malignite, a Family of Basic, Plutonic, ‘Orthioclase Rocks, Rich in Alka- | lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, by Andrew C. Lawson : : : Price, 20 No. 13. Sigmogomphius Le Dirke New Castoroid Rodent, from the Pliocene, near : Berkeley, by John C. Merriam . ni Price, I No. 14. The Great Valley of California, a Criticism. of the theory of Isostasy, ne Ar aia F. Leslie Ransome . Fi ; . Pricey abc ea VOLUME 2. ‘ th No. 1. The Geology of Point Sal, By Harold W. Fairbanks De pBrice: 65c No. 2. On Some Pliocene Ostracoda from near pagal by Frederick Chap- man . Price, Ice No. 3. Note on Two Tertiary Faunas from the Rocks of the Southern Coast of ; Vancouver Island, by J.C. Merriam . / oF Pricey No. 4. The Distribution of the Neocene Sea-urchins of Middle "California, and Its Bearing on the Classification of the Neocene Formations, by John Merriam 5 AW (itt Price, (oc No. 5. The Geology of Point Reyes Peninsula, by F. M. Anderson : . Price, No. 6. Some Aspects of Erosion in Relation to the ‘Theory of the Peneplain, by W. S. Tangier Smith : ea No. 7. A Topographic Study of the Islands of Southern Dicortes by. WwW Tangier Smith No. 8. The Geology of the Cental Portion of the Isthmus of Panama, by: Ose Hershey A P No. 9. A Contribution to the Geology of the John Day Basin, by John CG "Merriam Pric No. 10. Mineralogical Notes, by Arthur S. Eakle 5 No. 11. Contributions to the Mineralogy of California, by Walter C. Blasdale P No. 12. The Berkeley Hills. A Detail of Coast Range ig pia eee ee c son and Charles Palache p : ; UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 14, pp. 277-290, Pls. 28=30. ANDREW C. LAWSON, Editor < { ‘ THE PLIOCENE AND QUATERNARY CANIDAE OF THE GREAT VALLEY OF CALIFORNIA. BY JOHN C. MERRIAM. : CONTENTS. PAGE MEMEO GUC TION F222 cee nc 2 ences ceze center st Henendeeesoneece eer eres Ce eae ee 277 Hyaenognathus pachyodon n. gen. and sp. 278 Generic characters Fe ae cra es, OE LO, @GCCURTON CC) ooo cc ecoccececete es cesceesare se sesdeceseueveessses see tacton oo eee oe 279 JS TES ya 6 BT) ol ey Sa ee eee a eRe pene erese A) ND) Ta HH OND Se ees eee oa cece eect ecto eee, Coc ecaeeantessnc:20.cacaceevees ee 279 PAGE ANNNIGY GS frccctacencceces cesses each seneeen Meee cutee hee oc scutes St ecice ete ete OP (0) : IMC SIGUE GS fees ve eetee see ceca ss ee sega e eet geese eet ecco ceseecsa ee 283 Hyaenognathus? (Porthocyon n. gen.?) dubius n. sp. 0 283 WiStimetivie: Characters. 5 eye eee ee eee 283 Oeceurrence 22... ee eee Bcc My WA eo one eae a oe 283 (ONG ADRUT Ta eee ee oe ee ee no RO et ee Pr ee et eae Ae 284 Dentition Pe Sen Sen a ee OA ci Affinities 0.000... Defeat es BD See Pe, Sap RS a LE ESR EEE ARR eee eee 285 IME RSTUTCMMONCS: 2.25.22... 02e ees ceceek ccc ceeeeceesevseccceceees Dee eee ee eee, See 288 @amisiimdvamensis: Wevdiy: 2522.2. esee 2ecceec eee ccsacececeee ce ccceteevecee steseceess ee eee (OTE OV 61 ee ge 288 JESSE RMON ANS) ANT OY) oe ee eee ee ee, 289 INTIS ASTM YIU CMG ees seceeeeet cece sce sceceee cies eee ceusedecees eee see ¥cceedceee-ctecreeeeeeacv-aceeeeeesenee, 289 COE IRAN TIGER ANS) SJE Ty 2 E2)) oe ce re 290 INTRODUCTION. ‘ Up to the present time only two representatives of the Canidae have been known to occur in the Tertiary and Quaternary form- ations of California. One of these is supposed to have been found in Quaternary gravels at Murphys, Calaveras County, 278 University of California. [Vor. 3. and has been referred by Leidy to an existing coyote, Canis latrans Say. The second species was obtained from loose gravels near Livermore Valley, Alameda County. It was represented by a lower jaw which Leidy identified as Canis indianensis, a form deseribed by him previously from remains discovered in the Ohio Valley. Unfortunately, the Californian type has dis- appeared and we have only Leidy’s figure for comparison. Of the three specimens described in this paper, two were presented to the University of California some years ago. Shortly after they were received, the descriptions and figures published here were prepared by the writer. They were with- held from publication as the specimens were found to represent new and very peculiar types, a thorough understanding of which would necessitate the acquisition of additional material. During the eight years that have passed since these specimens were first studied, extended investigations of the gravels have been made but no new material has been discovered. As yet no very productive beds have been discovered in the fresh water Tertiary and Quaternary of California and the number of mammalian specimens found is small. It is to be hoped that somewhere in the extensive areas covered by these deposits in this state spec- imens may yet be discovered which will show other portions of the skeletons of these peculiar forms. A third specimen discussed here is referred to Leidy’s Canis indianensis, already described from this state. It is, however, of considerable importance. Since the loss of the jaw from Alameda County, it is the sole representative of the species known from this region. This specimen is in the museum of the California Academy of Sciences. Through the kindness of Mr. L. M. Loomis, director of the museum, and of Mr. F. M. Anderson, in charge of the palaeontological collections, the writer has been accorded the privilege of describing and figuring it here. HYAENOGNATHUS PACHYODON n. gen. and sp. Pu. 28, Figs. 1 AnD 2. Generic characters.—Mandible short and massive. Alveolar margins greatly flared below Ps and Pr. Dentition 3, T, 3, 3. Pz and Pz small. Ps molariform. Py very large, conical, MERRIAM. | Pliocene and Quaternary Canidae. 279 without accessory tubercles. My massive; protoconid and para- econid forming a heavy shear, metaconid absent; heel short, with reduced hypoconid and entoeconid. Mz and Mz small. Occurrence.—The type specimen of this species consists of a mandible (No. M8139, Univ. Calif. Palaeont. Mus.) found at Asphalto, Kern County, close to the foot of the Temblor Range. It was presented to the University by Mr. Bernard Bienenfeld of San Francisco. The excavations at the locality where the jaw was found seem to have been in beds ranging from late Miocene to Quaternary, but principally in the latest formation. A jaw of a large species . of Smilodon associated with the Hyaenognathus mandible indicates that it was probably obtained from a Quaternary bed, or possibly from the late Pliocene. Mandible.—The lower jaw is short and heavy, having a strong resemblance to that of the hyaena. Below the molars its height and thickness are about equal to that in the hyaena, but the anterior portion below the premolars is somewhat higher and heavier. As in the hyaena, the inferior border of the mandible is strongly convex below the posterior end of the molar series. Owing to the extreme shortness of the jaw, the alveolar margins are strongly flared below the carnassial and the last two premolars. The extent of this spreading possibly exceeded that in the hyaenas. Dentition.—The dentition contains a most remarkable mixture of primitive characters with some extreme specializations. The formula 3, +, 3, 3, shows the loss of but a_ single tooth, Pr, while the efficient portion of the dentition may be said to consist of but three teeth, a fairly developed canine, a powerful Py and a still heavier Mr. The incisors are missing from both rami but the clearly defined alveoli show that they were small and crowded. Iv and Iz were near the size of the corresponding teeth in the hyaena but Iz was much more reduced. The lower canines are short and stout and appear a little weaker than in the hyaenas. Of the three premolars, Pz has been lost but its alveolus shows it to have been a thick, single-rooted tooth somewhat 280 University of California. ° [Vor. 3. smaller than the one behind it. The root of Pz exhibits a deep groove near the top and was probably divided toward the lower end. The molariform crown seems to be somewhat worn but the button-like base is very thick, with a transverse diameter almost equalling the longitudinal. Pz has nearly two and one half times the antero-posterior extent of Ps. The simple cone of the crown has no anterior or posterior accessory tubercles, although there is a shelf on the cingulum at the posterior inner angle. On both rami the crown of this tooth is bent backward slightly and is very close to the anterior blade of the carnassial. In the molar series, M7 is exceedingly massive and with Py has done practically all of the work falling to the cheek teeth. The protoconid and paraconid are both greatly developed. No trace of a metaconid is discovered, although the postero-internal ridge of the protocone is prominent. The small talonid supports an external and an internal tubercle, both of which are very small and low. The crown of Mz bears an anterior and a poste- rior tuberele, of which that representing the talonid is much the smaller. Mz is represented by a small alveolus on each ramus. Affinities. —The dentition of Hyaenognathus has a striking resemblance to so much as is known of the problematical genus Borophagus, described from a jaw fragment found in the Blanco beds of Texas. For comparison Cope’s figures* of the type spec- imen are reproduced here together with outlines of the correspond- ing portion of the Hyaenognathus jaw (figs. 1, 2, 3, 4,5). The only other specimens referred to Borophagus are an inferior pre- molar with a conic basal cusp and a single blade of a sectorial, which were thought by Cope to belong here. If the premolar with a conie basal cusp belongs to Borophagus, the Californian form could not be closely related to this genus. If this is eliminated as doubtful and a comparison made with the type, we find the two forms possessing a combination of characters not found elsewhere. Both have the reduced Pz, depressed Ps, and the greatly enlarged, simple Py. Cope’s restorations of Pz in fig. 2 and fig. 4 show the posterior basal lobe of this tooth considerably extended. According to his view of the tooth in fig. 5, this * Geol. Sury. Texas, 4th Ann. Rep., 1892. Vert. Palaeont. Llano Estac. p. 52, Pl. XIII, figs. 4, 4a, 4b. Merriam. ] Pliocene and Quaternary Canidae. 281 restoration is not justified, as the outer portion of the heel was unbroken. On fig. 4 the writer has indicated in an unbroken line a third suggestion as to probable form, beginning the rest- oration at the point « where the break in the heel occurs. This shows the tooth to have a form somewhat similar to that of Pr in Hyaenognathus, although not so broad. Cope classified Borophagus on the assumption that it had four inferior premolars, though he suggests doubt of this at one point in his deseription. This is, however, improbable, as the presence of a Pr corresponding in size to what he considered as the large Ps and accompanied by a heavy sectorial would mean the elimina tion of Pr, just as has oeeurred in Hyaenognathus and in the hyaenas. Figs. l and3. Hyaenognathus pachyodon, < %. c, alveolus of canine. Figs. 2,4 and 5. Borophagus diversidens Cope, < %. c, alveolus of canine. a, point on P; where fracture begins. (After Cope.) Hyaenognathus is evidently allied to Borophagus and it is not impossible that future investigation may show generic identity. The differences in the minor details of form in the premolars indicate, however, that the types are specifically quite widely separated, Hyaenognathus being the more specialized. Several 282 University of California. (Vor. 3. facts suggest that, while we may show that the two forms are clearly related, we are not in a position to demonstrate generic identity. The Californian specimen represents a more extreme form coming probably from Quaternary beds, while Borophagus is Phoeene; the two occur at localities geographically distant from each other; and we do not know the most essential parts of the structure of Borophagus. The genus Borophagus was referred provisionally to the Hyaenidae by Cope, and the general form of the mandible in Hyaenognathus reminds one very much of that family. The dentition of Hyaenognathus has, however, no real structural resemblance to that of the hyaenas, though its functions were evidently similar. This genus represents a type analogous to the hyaenas, but is derived from a different source and worked out on a very different type of tooth structure. It represents the extreme of known specialization of the dog family in one direction. The genus differs so far from any known form that its affinities are not clearly shown. It resembles the Amphicyonine canids in the heavy jaw and simple premolars, but differs greatly in the characters of the tubercular molars and of the heel of Mi. Also, Py, although simple, does not correspond to any form found in the Amphicyonines. The genus Cephalogale, asomewhat primitive form referred by Zittel to the Simocyoninae, presents many points of resemblance, though it is separated by differences of the same nature as those just mentioned. Cninaat ee, ee, etre eremreveee" “THE UNIVERSITY PRESS __ FEBRUARY, 1904 __ £ PRICE 65 CENTS Os Pale eae ei hy EO ie : ¥ THe eta OF THE DEPARTMENT ¢ OF GxoLecy OF THE Uw: IVERSIT i YF per volume i is placed at $3.50, Thomas postage. The papers inte c will be sent to subscribers in separate covers as soon as issued. The separate n ‘may be purchased at the following prices from the University er a . sic whom remittances should be addressed:— <, ree Y 7, INN VOLUME 1. es , No... 1. The ‘@entony, of Carmelo Bay, by Andrew C. Kdveon, with cheeaead shale i ses and codperation in the field, by Juan delaC. Posada. ‘Price, 2, No. 2. The Soda-Rhyolite North of Berkeley, by Charles Palache i) Van ePrice ioc No. 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome wo). Briges 4oc | No. 4. The Post-Pliocene Diastrophism of the Coast of Southern California, by ih Andrew C. Lawson 5 Price, 4c 5 No. 5. The Lherzolite-Serpentine and Asegunita Rocks of the Potreo, San Reote ten say Francisco, by Charles Palache s CONGRATS No. 6. Ona Rock, from the Vicinity of Berkeley, ‘containing a New Soda P cone BP Py Amphibole, by Charles Palache - . a is No. 7. The Geology of Angel Island, by F. Leslie Ransome, ‘with a Note on the — ‘ Radiolarian Chert from Ahgel Island and from Buri-buri Ridge, San jee a Mateo County, California, by George Jennings Hinde i : rice; Asc twee No. 8, The Geomorphogeny of the Coast of Northern California, by Andrew C. as 4 Lawson : . © Price, 30c - Sa No. 9. On Analcite Diabase from San Luis Obispo County, California, by Harold ie 2) v ; W. Fairbanks . . Price, 25c oe Be, Nose, On Lawsonite, a New Rock- forming Mineral from tie Tiburon Peninsula, PA) Re ; Marin County, California, by F. Leslie Ransome . 3 - Avo BILGE, ROC A, ‘ No. 11. Critical Periods in the History of the Earth, by Joseph Le Gone ot, PEGE e aoc Ah x NS Me _ No. 12, On Malignite, a Family of Basic, Plutonic, ‘Orthoclase Rocks, Rich in Alka- lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, tention ue by Andrew C. Lawson. - * Price, 20 swe} No. 13. Sigmogomphius Le Contei, a New Castoroid Rodent, from ‘the Pliocene, ear errs Dyk Ag poe Berkeley, by John C. Merriam. ice, Ioc _ ie py _No. 14. The Great Valley of one a Criticism of the Theory of Isostasy, , "BY arse F. Leslie Ransome . : : 2 Paes 45c ‘ ree ar ve ‘VOLUME. 2. ees a WNo er. The Geology of Point Sal, By Harold W. Fairbanks : . . Price; 65c. / mee No. 2. On Some Pliocene Ostracoda from near Berkeley, by Frederick ‘Chap- Ne ae man . ‘Price, roc ye ge No. 3. Note on Two Tertiary. Funes from “the Rocks ‘of the Southern Coast of Faas Vancouver Island, by J.C. Merriam . 1 Reices toc No. 4. The Distribution of the Neocene Sea-urchins of Middte California, and Its nt Bearing on the Classification of the Neocene Formations, ie ai Ce aN Merriam f / ; Price, oe A No. 5. The Geology of Point Reyes Peninsula, by F. M. Anderson” . 1 Priced af No. 6. Some Aspects of Erosion in Relation to the Theory of the Peneplam by W. iSratd _S. Tangier Smith < cat Price, 2 2c “No. 7. A Topographic Sida, of the Telands: of Southern California, by Ww, So voy f e Tangier Smith | 5 pi Prices 4oc ue No. 8. The Geology of the Conta Portion of ‘the Isthmus of Se bye 1st, * Hershey e » yt No. Io. Winer alonical Notes, by. “Arthur Ss. Bakle mae abr No. 11. Contributions to the Mineralogy of California, by Walter C. Blasdale No. 12. The Berkeley Hills. A Detail of Coast Rane Geology, ‘bys ierein a ‘son and Charles Palache . : ek UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 15, pp. 291-376, Pls. 31-45 ANDREW C. LAWSON, Editor THE GEOMORPHOGENY OF THE UPPER KERN BASIN ihe ANDREW C. LAWSON. CONTENTS. Mmtroductvom) 2. ............ ot cesses ccc ecceeeeeee Petrographie and Structural Features «02.2.0... 2.0. eck cece ee neeeeeeeees ceeeeeeees Roeks and Geomorphy (Cine wout ake, eos ee ee eS Quaternary Lavas ....... 0.2... eeceeeeeeeeeees cee The Roof of the Granite ......... A aoe Jointage...... : Faults and Fissures The General Relief and Drainage _......... The High Mountain Zone Kaweah Peaks and the Mineral King Belt Mee) jefe amb oath Ky op a0 UME eee ee mene ec oP sp rp OO : The Sub-summit Plateau 2.00.0 20000 0... Other Plateau Remnants... 0... Sculpture of the High Mountain Zone Significance of Upland and Plateau _.. MUU eWey 1S veal oty \W/fat) DW = A Aho asta ee nea ra Chagoopa Plateau ................... Moow~ay Vial ey 2 sees eee Gee ec: The Little Kern Plateau ............0......... Former Connection of High Valleys AM aYey (Chewovoy ol. /A oso) 2 ee ee Kern Canon and Crustal Rifting .. Kernbuts and Kerneols 0.0.00... Possible Explanations 0000000... f Landslide Hypothesis 00000000. Rift Hypothesis.............. Le rd, : 292 293 293 294 296 297 298 300 301 302 304 305 307 307 308 309 310 312 315 315 319 325 327 328 331 331 333 334 336 292 University of California. [Von. 3. Harmony of Kern Canon with Rift Hypothesis _ 336 The Trout Meadows Defile..000 000... ; : Been cris) Application of Rift Hypothesis to Kernbuts...... ae .. 840 Final Statement of Hypothesis _. ee 341 Application to Kern Canon _.... : ee eeer a _ 342 The Kern Lakes ........ ee sere? ~ : ae a OLS! Glaciation Cr Te Pe re er ae Pres See AO LO) Terminal Moraines of the Trunk Glacier Seon . 345 Glacial Modification of Kern Canon ....... LOY cao tge dy 349 Tributary Glaciers ...... ae peers Ou) Glaciation of Outer Border of Basin... ....... eer eee .... B54 Cirques.. .. a see aereesis Ba eee 357 Historical Argument and Resumé ee sh eS occa 362 Appendix .......... pecans sdiees MEAS 25 Weghtss accra dbawat sestianags totoceSeeees!steiiive leans: coach eee OOO INTRODUCTION. During the past season the Sierra Club held its annual outing in the basin of the Upper Kern River. In the large party of enthusiastic mountaineers who participated in the excursion were two geologists. One of these was Mr. G. K. Gilbert and the other was the writer of this paper. Both were attracted by the opportunities which were afforded by the Club’s program for exploring, from a geological point of view, this little known but highly interesting portion of the Sierra Nevada, and at the same time indulging in a few weeks of exhilarating recreation. The observations, upon which the present sketch of some of the geological features of the region is based, were made to a large extent by both Mr. Gilbert and the writer while travelling together over the mountain trails and climbing the peaks that served as vantage points, from which we looked down upon and viewed, aS a map spread at our feet, the country through which we passed. The interpretation of these observations was a com- mon theme of conversation both at the time they were made and in camp. Under these circumstances it is evident that a large share of whatever merit this sketch possesses belongs to Mr. Gilbert. In so far as it is desirable that the common observa- tions should be made a matter of record, it would have been better for geological science had the writing of this paper been undertaken by Mr. Gilbert; but he, pleading pressure of more important work, has generously waived the rights of authorship Lawson. ] The Upper Kern Basin. 293 in this field, and so imposed upon the writer the task of narrating and discussing the observations made upon the trip as best he may. But while gratefully acknowledging Mr. Gilbert’s cooper- ation in the field the writer has, thereby, no intention of throwing upon him the onus for the shortcomings of this discussion. That responsibility rests with the writer. It is needless to say that neither the record nor the discussion pretend to exhaust the geology of the Upper Kern Basin. The region is replete with geological interest and only some of the more salient problems are taken up; and even these suffer from the partial character of the exploration of the region. The basin of the Upper Kern presents features of exceptional interest to geomorphologists, and the purpose of the paper, as its title implies, is to outline these features and discuss their genesis. While the paper professes to deal primarily with the basin of the Upper Kern, certain features of the region immed- iately adjoining it are incidentally referred to by way of supple- menting the account of the basin itself. A brief description of the rocks of the region, in which petrographic technicalities ave dispensed with as far as possible, is given at the outset of the paper as a necessary introduction to the subject matter. The conelusions to which the discussion leads have a general bearing upon the historical geology of the Sierra Nevada, and this bearing is indicated at the close of the paper. The illustrations, when not otherwise indicated, are from photographs by the writer. The map is based on the blue print compilation by Professor J. N. LeConte. All new altitudes are based on barometric measure- ments made by Professors J. N. LeConte and A. G. MeAdie. PETROGRAPHIC AND STRUCTURAL FEATURES. Rocks and Geomorphy.—Fundamental to the understanding of the geology of any region is a knowledge of the rocks which underlie it. Especially is this the case when the problems with which we have to deal are those of geomorphogeny such as concern us very largely in the discussion of this region. It will, therefore, be appropriate to first state briefly the general petrographic characteristics of the basin and of such portions of the neighboring territory as may be conveniently discussed in connection with it. 294 University of California. (Von. 3. The rocks which underlie the hydrographic basin of the Upper Kern are almost wholly granitic in character. This is a fact of prime importance for the study of the geomorphic evolution of the region. The relief as determined by general atmospheric, stream, and glacial erosion has been controlled by the uniformity of the materials subject to seulpture by these agencies. It has been uninfluenced by that marked differentiation of structure and of resistance to erosion which characterizes the stratified rocks whether they be detrital or volcanic, unaltered or meta- morphic, horizontal or folded. There are no belts of soft rocks which might have been sought out by enterprising head-water streams, and by these exploited till they became the dominant drainage lines of the region; no belts of hard roeks which might have been left as dominant ridges; no superposition of hard rocks upon soft which might have yielded mesas and serried escarpments. Yet the region is one of the boldest possible relief. The altitudes within the basin have a range of over 8000 feet. There are very striking contrasts in the slopes of the basin. There is a pronounced system in the drainage lines; and the master stream of the basin, the Kern itself, has a course as straight as an arrow for nearly its entire length. These facts indicate clearly that, notwithstanding the nearly uniformly granitic character of the region, there has been a certain direc- tive control of its seulpture due in part to the character of the rocks. If, with this conclusion in mind, we turn again to the rocky floor of the basin and attempt to characterize it more precisely we find facts which to some extent, at least, justify it. Granitic Rocks.—In the first place it may be stated that even where the rocks are granitic, even in the strict sense of the term, this granite presents considerable variation in character. In the middle of the basin, along the canon of the Kern, the rock is prevailingly a light-colored, coarse, very quartzose biotite- granite. This rock has frequently a porphyritic appearance owing to the exceptional size of the orthoclase crystals, but the latter are as a rule imperfectly formed and the structure would on the whole be classed as hypidiomorphie granular. This granite grades through varieties, in which hornblende replaces part of Lawson. ] The Upper Kern Basin. 295 the biotite, into hornblende-granite with much less quartz. From these there appear to be gradations into quartz-diorite and diorite in which plagioclase can be recognized easily in hand specimens. These more basic facies, however, appear to be quite subordinate in extent as compared with the common biotite-eranite. In this type of granite, dykes or veims of peg- matite are rare; but on the canon walls above the meadows there are numerous small dykes of a reddish, or flesh tinted, fine- grained granite, with but very little admixture of ferro-magnesian minerals. The rock may be perhaps conveniently classed with the aplites, although its structure, as judged by hand specimens, appears frequently to be granular. These dykes were observed in several instances to be from three to five feet wide, but the width of most of them probably does not exceed one foot. They appear to have had little or no influence in giving direction to differential erosion. The biotite-granite of this portion of the basin, together with its dioritie facies, is characterized by the presence of a great abundance of angular, sub-angular and rounded inclusions of a darker gray, finer grained, porphyritic rock. These appear usually to be shghtly more resistant to disintegration than the granite which holds them. In some instances, where such inclusions are particularly abundant, it was estimated that there might be one ecubie foot of inclusion for every cubic yard of granite. On the average, however, where these inclusions oeceur, there is probably not more than one cubic foot of inclu- sion to every four or five yards of granite. In size the inclusions range from a few inches to several feet in diameter and probably average about one foot. In this biotite-granite there are, also, in the canon of the Kern comparatively small areas of coarse-grained gabbro-lke rock, in which, however, the proportions of feldspar and ferro-magnesian silicate vary. This gabbro may be assumed, in the hght of eurrent doctrines on magma differentiation, to be genetically connected with the granite; but the transitions from the gabbro to the granite, so far as they were observed, are abrupt, and more suggestive of an intrusive relationship than of a gradual transition of one rock into the other. These gabbro areas are 296 University of California. [Von. 3. devoid of the inclusions which abound in the adjacent granite. The gabbro, where exposed to the weather, shows the etching of the feldspar and the relief of the pyroxene. Dykes.—In addition to these more intrinsic characters of the granitic rocks in the vicinity of the canon of the Kern, it may be stated that near the Kern Lakes and for some little distance above Coyote creek the granite is cut rather frequently by small dykes of black, fine grained lamprophyre. These are rarely more than a few feet, sometimes only a few inches, in width, and have all attitudes from nearly horizontal to quite vertical. Some of them are multiple dykes. These dykes appear to be particularly abundant on the east side of Kern Canon below Lower Lake, on a sear formed by a great rock-slde, where they dip northeasterly at low angles. The dykes above the mouth of Coyote Creek strike E.N.E. and dip southerly at an angle of 70° from the horizon. A multiple dyke of three members was here observed. The most northerly is from four to five feet wide; the next parallel dyke to the south, 10 feet distant, is about two and a half feet wide; and the next, about 10 feet farther south, is six inches wide. The rock is here a dark gray, porphyritie rock with phenoerysts of feldspar and hornblende, the latter predominating. The groundmass is fine grained but apparently holoerystalline. The texture on the chilled edges against the granite is finer than in the middle of the dykes. A little to the south of this multiple group another dyke of the same rock was observed with a strike at right angeles to that above recorded. These dykes are somewhat more resistant to the weather than the granite which they cut, and are, therefore, somewhat prom- inent as a shoulder on the steep mountain slope. They break down into angular blocks, while the granite on disintegration crumbles to a coarse sand, Such dykes, though locally abundant in the southern part of the basin, in the Kern Canon, do not appear to be at all common throughout the basin and cannot be said, even where they abound, to have exercised an important influence upon the gen- eral morphogenic process, by determining lines of either maxi- mum or minimum erosion; unless we assume that the association of an exceptional number of such dykes with the large rock-slide Lawson. ] The Upper Kern Basin. 297 below the Kern Lakes is more than a coincidence, an assumption which the writer does not feel warranted in making. Except for the occurrence of the gabbros and the lamprophyric dykes, the summary account given above of the granitic rocks of Kern Canon would apply fairly well to all the granite country lying to the west of Kern River in so far as it came under the writer’s observation. In the high country to the east of Kern River, however, particularly in approaching the summit crest, the granite has quite a different facies. The rock here is uniformly a light colored biotite-granite with a splendidly devel- oped porphyritie structure. The porphyritie crystals are huge orthoclases with perfect crystal boundaries. These are quite frequently three inches in length and average two inches over wide areas. They usually contain inclusions of biotite and hornblende, disposed in rude rectangular zones parallel to the planes of growth of the crystal. In this granite there appear to be no loeal basic facies, and the inclusions which are so abundant in the granite of the Kern and the country to the west are almost or wholly absent. Dykes of coarse pegmatite are fairly common; and dykes, often of large size, of gray and pinkish aplite are in places very abundant. Disintegration.—These purely petrographical differences in the prevailing rock of the region are mentioned for the purpose of indicating possibilities in differential resistance to erosion and so aiding us in coming to an understanding of the inequalities of the relief. That such differential resistance to the attack of atmospheric agencies actually does characterize the granite, even where no petrographiecal distinction can be drawn, is amply witnessed by the heavy mantle of disintegration products which occurs upon many of the unglaciated slopes, sometimes as a coarse, loose sand into which one sinks deeply in climbing, and sometimes as an eneumbrance of loose blocks of large dimen- sions. The disintegration which yields the coarse granitic sand is well exemplified on the trail between Farewell Gap and Coyote Pass, on the upper waters of Coyote and Voleano Creeks, and along the trail between Mt. Guyot and Crab-tree Meadows. On the steep upper slopes of Sawtooth Peak and Mt. Whitney this sand is very abundant, but is in such situations admixed with angular 298 University of California. (Vou. 3. blocks of comparatively fresh granite. The summits of the high peaks, whether flat topped as in the case of Mt. Whitney, or acutely pointed as in the case of Sawtooth, are characteristically encumbered with large angular blocks of granite almost or quite free from finer fragments or sand. These larger blocks present the appearance of having been detached from the underlying surface of granite by a process of decrepitation without the intervention of any appreciable rock decay. It is a process of denudation which has been operative very generally on the high summits of the Sierra Nevada and, indeed, on similar peaks in various parts of the world, as, for instance, Pike’s Peak in Col- orado, and Ben Nevis in Seotland. But while the encumbrance of angular blocks of fresh granite is characteristic of the high sum- mits and is without doubt due to certain peculiar conditions which obtain there, the tendency to secular decay, which yields the granite sand, is by no means uniform. Large areas of the unglaciated surfaces, even when these are of gentle slope favor- able for the accumulation of such sand, show but little of it; while other areas of the same rock, even where the surface is so steep that the sand lies at the angle of repose of loose material, are deeply buried by such waste products. We have in this fact an indication of differential resistance to atmospheric erosion which does not appear to be suggested by the usual petrographic characterization of the terrane, although doubtless the causes for the difference of behavior under the weather could be revealed by sufficiently thorough petrographic investigation. Kaweah Peaks and the Mineral King Belt.—It must be noted, also, that certain limited portions of the Upper Kern Basin are not composed of granite, and that at least one notable feature of the relief is due in no small measure to this exceptional character of the rocks. The bold group of the Kaweahs (Plate 338), which extends southeasterly into the basin from its western rim, has a certain individuality and character which distinguishes it from all the other mountain peaks, either in the basin or on its rim. The rocks of this group appear to be metamorphic sediments judging from the similarity of their appearance to such rocks in the Mineral King metamorphic belt, in which occur vari- ous crystalline schists, clay slates, quartzites, and limestones. Lawson. ] The Upper Kern Basin. 299 These rocks are for the most part distinguished from the granite, even at a distance of many miles, by the rusty, reddish brown color which they assume under the weather, and by their smoother and more conical profiles. ; Isolated areas of such metamorphic rocks appear to be by no means infrequent in the granites of the southern Sierra Nevada, and, as our knowledge of them is but scant, if may be well to here say a word about the occurrence at Mineral King. This belt has a width from east to west at Mineral King of about four miles. Its western limit against the granite is observable on the eanon walls of the East Fork of the Kaweah a mile or less below Mineral King. Its eastern limit is splen- didly exposed in the fine glacial cirques which lie to the south- west, west, and northwest of Sawtooth (Plate 43, 4 and B). These contacts show clearly that the granite is intrusive in the ‘sedimentary rocks. The metamorphism of the latter is referable to thei contact with the granite. On both sides of the belt which lies within these limits, the contact plane is in general nearly vertical, but in some places on the eastern edge of the belt it dips to the east so that the granite is resting upon the sedimentary rocks. This contact is observable again to the east ot Mt. Florence and on the mountain slopes to the east of Bullion Flat on the Little Kern. From this point the belt may be fol- lowed down the canon of the Little Kern, on the west side, for about four or five miles, but appears to be very much narrower than at Mineral King and eventually tapers out. In its northern extension the belt may be followed over Timber Gap and across Cliff Creek, but does not cross the main stream of the Middle Fork of the Kaweah. Beyond Cliff Creek it must either pinch out rapidly or swing around to the northeast, cross the Great Western Divide, and connect with the similar rocks of the Kaweah Peaks, in the basin of the Upper Kern. Whether this connection now exists was not positively determined. It seems not improbable, however, that the rocks of the Mineral King belt and those of the Kaweah Peaks are parts of the same belt of strata. In the Mineral King belt, at least, we have a remnant of a once extensive pre-granite sedimentary terrane, which, in a sharply pleated and appressed condition, sank deeply into the 300 University of California. [Von. 3. granite at the time of the invasion of the crust by the latter in a magmatic condition; a remnant in other words of the roof of a vast batholith. The influence of this belt of stratified rocks upon the character of the stream topography is very apparent. The strata are inclined at high angles to the W.S.W. The canon of the east fork of the Kaweah, above Mineral King, and that of the Little Kern, flowing S.S.E. from Farewell Gap, follow the general strike of the strata and are good illustrations of well controlled subsequent drainage, modified, as will be seen later, by glacia- tion. This subsequent topography is in contrast with the drainage features within the basin of the Upper Kern, where no such control of stratiform structure exists. The limestones of this bed of metamorphic rocks afford the necessary conditions for the formation of underground channels of dissolution. On the west wall of the east fork of the Kaweah, a little above Mineral King, at an elevation of a few hundred feet above the bottom of the canon, a large stream issues from such a channel and falls as a beautiful cascade over a bank of travertine deposited from its waters. There are also extensive travertine deposits immediately below Mineral King, large enough to modify, in detail, the geomorphie profile of the valley and to deflect the course of the drainage. Quaternary Lavas.—There remains to be mentioned, in this review of the rocks of the region, certain voleanic roeks which have a quite limited distribution in its southwestern and southern part. These are the small volcanoes and lava streams of Toowa Valley, and the lava sheets to the south of Trout Meadows and elsewhere near the confluence of the Kern and Little Kern. These are basaltic in character. The voleanoes of Toowa Valley are of very recent date. The geomorphic evolution of the region had reached its present stage long before the voleanic vents opened. Their contribution to the general morphogenic history is confined to the addition of a few small cones to the relief, and to the obstruction by these, and by the lava streams that flowed from them, of the drainage of Toowa Valley (Plates 35.4 and B, 364). The lava sheets of the country at the confluence of the Kern and Little Kern are of less recent date, and yet they rest as a Lawson. | The Upper Kern Basin. 30] veneer upon plateau surfaces which represent a comparatively late stage in the evolution of the geomorphy of the region. In the later stages of that evolution they have suffered the same dissection as the plateaux, and appear now only as remnants. Where they remain, however, they greatly accentuate the flatness of the plateau, and this is their chief contribution to the general morphogenic process. From the foregoing statement of the petrographic character- istics of the terranes which underlie the basin of the Upper Kern, it will be evident that there are certain diversities in the rocks of the region which account in some measure at least for the inequalities of the relief in so far as these are due to atmos- pheric erosion. When, however, we ask what part these varying petrographic characteristics have played in determining the drainage scheme of the basin, there is no answer forthcoming. Nothing in the petrography of the terranes affords us any clue, for example, to the arrow-like course and meridional trend of the master stream of the basin, and much less does it afford an explanation of the remarkable contrasts in the slopes of the basin. The Roof of the Granite.—It has been stated in the foregoing discussion that, in various parts of the granitic region of the southern Sierra Nevada, there are outlying areas of pre-granitic stratified terranes, remnants of formations which formed the outer crust of the earth in this region, at the time of its invasion by the vast Sierran batholith or batholiths. These formations may be safely assumed to have originally arched over this batho- hth as a covering shell. The surface of contact between the granite and the overlying rocks was clearly a very uneven one. This is shown, not only by the relation of these remnants to the granite, but also by the spacial relations of the granite and the rocks invaded by it in the northern Sierra Nevada, where the relative areas of the two classes of rocks are reversed and the granite appears as inliers in the stratified, though often highly metamorphosed terranes. It has been made clear farther that, in the Mineral King belt of sedimentary rocks, which lies imme- diately to the west of the Upper Kern Basin, we have such a remnant of the roof of the batholith which has been sunk deeply 302 University of California. (Vor. 3. into the granitic magma, and that in the Kaweah Peaks we have probably another such area, or, possibly, an extension of the Mineral King belt. The Kaweah Peaks area, however, appears rather to be sessile upon the granite than sunk down into it, although this is questionable. These facts suggest that over the granitie terrane of the Upper Kern Basin the original upper surface of the batholith may not be very far above the present actual surface, and that the two may, in places, be even coincident, the present surface being in such a case merely the original upper surface of the batholith stripped of its covering by the usual processes of denudation. Such a contact plane between a batholith and its roof would constitute a structural feature of no mean importance in the degradation of the region; and the possibilities of this control are considered in a subsequent portion of the paper. Jointage.—In many parts of the Upper Kern Basin the granite of the region exhibits a pronounced jointage. This structure is best displayed in the walls of the glacial cirques in the higher parts of the mountains, and is less abundantly developed in the walls of the deeper canons. In eases where horizontal jointage prevails there may often be seen distinet and striking differences in the spacing of the joint planes in a vertical range of a few hundred feet, on a cliff face. Near the top of the cliff the joint planes are close together and the joint blocks thin, while lower down they are more widely separated and the blocks thick. Similar differences in the spacing of joint planes have been observed by the writer in other parts of the Sierra Nevada, as for example in the walls of Yosemite. Such horizontal jointages are usually traversed by others approximately vertical, breaking the rock into more or less rectangular prisms or slabs. In other cases the granite has a sheeted or lamellar structure, due to the dominance of a single system of nearly vertical jointage. This is finely exemplified in the cirques about Mt. Whitney, where the sheets are thin and remarkably even from the top of the cirque walls to the bottom. But the direction of this vertically sheeted jointage is not constant over wide areas. In the cirque southwest of Mt. Whitney its strike is roughly east and west, while in the cirque northwest of Mt. Whitney its direction is Lawson. ] The Upper Kern Basin. 303 northwest and southeast. The horizontal and vertical jointages are the most regular and persistent, but there are many parts of the region where the joint planes have all attitudes except verti- ral and horizontal. In such cases they intersect without apparent system and are often distinetly eurved; and the intensity of this jointing is, also, characteristically much more marked in the upper part of cliff faces than in the lower. Some interesting divergencies of joint planes were observed in the case of sharp crests between opposing cirques, in which the jointage in each cirque was parallel to the slope of its walls. In general no definite and persistent system of jointage can be said to charac- terize the region, the directions of all but the horizontal jointage varying greatly, and even that is only ealled horizontal by cour- tesy, for it is not uncommonly inclined at as much as 10° or more to the horizon. But there appears to be a more or less definite relationship between the intensity or frequency of joint- age, particularly horizontal, oblique and curved jointage, and proximity to the high surfaces of the region, and a similarly close relation between the oblique or curved jointage and the form of the surface. If this general proposition be true, and it certainly has an observational basis, then the jointage would appear to have been developed in part, at least, pari passu with progress of erosion, and to be, in a sense, dependent upon it. If this be the case, then jointage in these granites cannot be a structural feature altogether antecedent to the geomorphic evolu- tion and so controlling the latter. They cannot, therefore, be supposed to be due to compressive stresses in the rocks according to the current doctrines on the subject, but rather to tensile or expansive stresses arising from the relief of load as affected by erosion. The stresses in mountain masses due to simple gravity, as discriminated from tangential compression, which is of course itself a phase of gravitation, are very great and become com- plexly distributed as the region undergoes dissection. The balanee of stress is destroyed in proportion as the surface is uneven and asymetric, and an elastic tension is developed near the surface, which is relieved from time to time by the rifting of joint fissures. This hypothesis, explanatory of jointage of granites in the High Sierra, may not be of universal applica- 304 University of California. [Vor. 3. tion; * but it seems worthy of consideration as an alternative to the at present more favorably received hypothesis, which explains jointage as a result of tangential compression, entirely independent of, and antecedent to, erosion. This hypothesis of jointage as entertained by the writer modi- fies the views, which might otherwise be entertained, as to the role which this structure has played in the general morphogeny of the Upper Kern Basin. If the jointage were strictly an ante- cedent structure, simply revealed by erosion, then we should expect it to exercise an important influence upon the direction of the maximum erosion lines; and this may be true of the vertical jointage. But if the jointage be a function of erosion to any extent, then the control exercised by jointage upon the course of erosion 1s correspondingly diminished. Nevertheless, since joint- age is developed in the rock mass in advance of the surface due to erosion at any given time, it greatly facilitates erosion, whether the latter be effected by atmospheric, stream, or glacial agencies. The relation of the relief to the jointage of the region would require a careful, detailed survey, and no more positive statement can at present be made concerning it. Faults and Fissures.—No notable faults have been detected in the Upper Kern Basin, but in view of the homogeniety of the rocks this is not surprising, and they may easily exist. Faults are usually made apparent by the discordance of the rocks on either side of the plane or zone of dislocation; but in the case of massive granites such discordance is not in evidence and they escape detection. The character of the eastern rim of the basin is, it is scarcely necessary to say, due to the great fault which limits the Sierra Nevada on the east. The east front of the range is a fault scarp which has been modified by degradation, and in its upper part been accentuated in sheerness by cirque erosion. As will appear in the part of the paper dealing *Mr. G. K. Gilbert kindly reviewed the MS. of this paper and has communi- cated to the writer his opinion that only the curved jointage parallel to the surface may be hypothetically explained in the way here suggested. It must be confessed that the statements which are made of the horizontal, oblique and curved jointage cannot be urged with the same force with reference to the vertical jointage, par- ticularly in the sheeted granite. The writer, therefore, does not here attempt to apply the hypothesis to the vertical joints, although he believes that they also are due to expansive stresses and not to compression as ordinarily held. Lawson. | The Upper Kern Basin. 8305 with Kern Canon, there is strong inferential evidence that the canon follows the line of a rift fissure, and in connection with this fissure there has been a certain amount of minor faulting. THE GENERAL RELIEF AND DRAINAGE. In attempting to form just conceptions of the relief of the Upper Kern Basin the best, and probably the only satisfactory, method to be followed is to look down upon it from some of the high peaks which command it. The only alternative capable of yielding similar results would be to study the region from the basket of a balloon: but that has its drawbacks. Moved by this doctrine, several of the more commanding points situated either on the rim of the basin, or within it, were occupied and very comprehensive views obtained. The best of these for the study of the relief are afforded by the summits of Mt. Whitney on the eastern rim, Sawtooth on the western, and Mt. Guyot in the more central portion of the basin. Perhaps the finest view of all, judging from its situation, would be that from Kaweah Peak; but this was not occupied. A very impressive view of Kern Canon is obtained from the summit of Tower Rock, which rises sheer from the river 2150 feet just opposite the mouth of Coyote ereek; and from the voleanie cones of Toowa Valley the charae- ter of surface of the unglaciated region of the southern Sierra Nevada may be studied to great advantage. The observations made from such points of view, supplemented by others upon the character and form of the surface made at closer quarters, have led to certain definite impressions as to the configuration of the Upper Kern Basin and of its geomorphic evolution which it is the purpose of the present paper to set forth and discuss. The Upper Kern down to the point where it is joined by the Little Kern drains a hydrographic basin of about 400 square miles. This area when delimited upon a map* is seen to be oval or leaf-shaped, the north and south diameter being 35 miles and the ereatest east and west diameter 16 miles (Plate 31). The drain- age scheme is like the veination of a leaf, the trunk stream of the Kern flowing due south with a remarkably straight course as a midrib through the center of the area. On either side tributary * LeConte’s blue print “Map of a portion of the Sierra Nevada Mountains, No. 3, Kings-Kern Sheet,” is the best map of the region. 306 University of California. [Vor. 3. streams flow into the Kern at short but irregular intervals. The more important of these on the east side are, in order from north to south, Tyndall Creek, East Fork of Kern River, Whitney Creek, Rock Creek and Voleano Creek, and on the west side in the same order Kern-Kaweah River, Big Arroyo, Rattlesnake, and Coyote Creeks. The area thus drained is a pronounced basin in the morpho- logical as well as in the hydrographic sense. The rim of the basin is for the most part a chain of lofty peaks and mountain crests. On the west this chain extends from Table Mountain (13,625 feet) on the north, with a trend concave to the basin, to a point near Trout Meadows and is known as the Great Western Divide. It sheds the waters westward to the upper reaches of the Little Kern River, the East and Middle Forks of the Kaweah and the Roaring River branch of the King’s, and eastward to the Upper Kern. On the east the chain forms part of the main divide of the Sierra Nevada, the summit erest of the range, and separates the waters of the Upper Kern from those of the Great Basin. This divide extends from Junction Peak (13,916 feet) to Cirque Peak (12,941 feet) as a wonderfully bold mountain crest and includes Mt. Tyndall (14,101 feet), Mt. Whitney (14,522 feet), and Sheep Mountain (14,059 feet). The conjunction of these two great divides on the north, spanning the gap between Table Mountain and Junction Peak, encloses the Upper Kern 3asin in that direction, and separates its waters from those of Bubb’s Creek, a tributary of the King’s. South of Cirque Peak the watershed between the Upper Kern Basin and the South Fork of the Kern is a comparatively low divide, which leaves the summit erest about two miles southeast of Cirque Peak and thence converges upon the Kern River near its Junction with the Little Kern, following part of the way the somewhat subdued Toowa Range. This divide is depressed to the drainage line at its intersection by Toowa Valley, in which lies Voleano Creek flowing westward, and South Fork flowing southeastward. This is the lowest point in the rim of the Upper Kern Basin, excepting the main drainage outlet, and a remarkable depression to the north of Trout Meadows to be described later, and has an altitude of about 8600 feet. BUEES DERI GEOEMUINIVG CAL A St 3 ij a2 eee ceve ZALN \ N Kom JA Sag ues ak ‘J a ea bee ae Ilia i Ne mso ly A Ve Zz LEGEND F | High Mountain 4 Zone High Valley Zone ES Glacier Tracks 7) UPPER KERN BASIN VOR Sie Flees: ls DIAGRAM ADJACENT MOUNTAINS Showing the relation of the High Valleys to the High Mountain Zone and to the Sierran Canons; also the Limits of Glacia- tion of the Southern End of the Sierra | 2,° Lawson. ] The Upper Kern Basin. 307 At the base of the steep slopes of the high mountains, which thus encircle the Upper Kern Basin from the southern end of the Great Western Divide to Cirque Peak, there spreads out im the central part of the basin a broad valley land of very subdued relief. This valley land is known as the Chagoopa Plateau. From the mountains on either side of the basin it slopes gently with a remarkably uniform surface toward the Kern. Its upper limit at the base of the high mountain peaks and crests is about 10,500 feet, while its lowest part at the brink of the Kern Canon is from 8,400 feet in the southern part to about 9,000 feet in the northern part, above sea level. Through the central part of this high valley runs the profound canon of the Upper Kern, a meridional trough sunk in the valley floor to a maximum depth of about 2,500 feet and bordered by almost vertical walls for a large part of its course. The streams which drain the high mountains on either side flow through similarly deep, steep- walled trenches as they cross the Chagoopa Plateau on their way to the Kern, but in no ease have they cut as deeply as the master stream. It thus appears that within the Kern Basin there are three hypsometrie zones, distinguished by such marked differences in the character of their relief as to constitute three distinct geo- morphie zones. These may be called for convenience, (1) The High Mountain Zone; (2) The High Valley Zone; and (3) The Canon Zone. THE HIGH MOUNTAIN ZONE. The Summit Upland.—This zone has been characterized in the sketch of the rim of the basin as consisting essentially of high peaks and erests. This, however, does not sufficiently describe the geomorphic character of these mountains, and some of their more striking features must be noted particularly. Several of the culminating portions of the summit divide are either flat topped, or have slopes which are so gently inclined as to be in sharp contrast to the more precipitous slopes which abound in the region. The best illustrations of such flat, or gently sloping, summits is that afforded by the summit range from Sheep Mountain to Cirque Peak. The summit of Mt. Whitney itself is 308 University of California. (Vor. 3. nearly flat for perhaps half a mile square, with a very gentle slope to the west. This flat slope is surrounded on nearly all sides by precipices which are, for the most part, the walls of glacial cirques. Sheep Mountain (Plate 32.4), five miles south of Mt. Whitney, shows the same kind of a flat topped summit; but this merges by a simple curve into a westerly slope which is very smooth and even as viewed from a distance, but is much steeper than the summit of Mt. Whitney. Similar characters obtain along the summit divide as far as Cirque Peak, and por- tions of the flatter summits even slope easterly, at a slight angle, to the brink of the precipices on that side. The same surface is well displayed in a view from Mt. Guyot toward Mt. Whitney (see Plate 33.). In general, however, the westerly slope of this portion of the summit range in smoothly flowing, sometimes undulating, curves from the flatter summits is its most charaec- teristic feature. This smooth surface, where not interrupted by glacial cirques, descends to an altitude of about 11,500 feet, where it meets a splendidly defined plateau to be described shortly. It has thus a hypsometric range of about 3,000 feet. In this range the flatter portions of the slope are not confined to the highest summits. About half-way between the upper and lower limits there is a flat and quite broad terrace* which is best exemplified in the summit tract between Sheep Mountain and Cirque Peak. (Plate 324). Remnants of such a surface as that here deseribed are observable in various parts of the region. It is evidently a significant feature of the geomorphy of the Upper Kern Basin. For convenience of reference it is here named the Summit Upland, from the fact that its character is well typified in the summit of the Sierra Nevada from Mt. Whitney to Cirque Peak, and that in this part of the region more people will prob- ably make its acquaintance than elsewhere. The Sub-summit Plateau.—To the west of Cirque Peak the summit upland descends by insensible gradations to a well defined plateau which is best preserved in the country to the west and southwest of the Siberian Outpost. This plateau may be conveniently designated the Sub-swmmit Plateau. It is best * This term is used as one descriptive of the geomorphic form without implica- tion as to the origin of such form. View south and southwest from summit of Mt. Whitney. Showing remnants of the Summit Upland between Sheep Mt. and Cirque Peak. The destruction of this ancient upland by the development of glacial cirques is well shown. Tiew looking southeast and south from Mt. Guyot. Showing the Sub-summit Plateau on the right and the Rock Creek extension of the Chagoopa plateau on the left dissected by the U-shaped canon of Rock Creek. Hanging glacial valley above lateral moraine on right side. The slopes of the Summit Upland on the extreme left. Lawson. ] The Upper Kern Basin. 309 seen from the top of Mt. Guyot looking south and southeast. (Plate 328). A more distant view of it is obtained from the sum- mit of Mt. Whitney looking southwest. (Plate 33.4). From both view points it is seen to be a remarkably even and level surface partially dissected by glacial erosion. On its western border, immediately south of Guyot, a sharp but not high ridge rises above its general level, and similar higher ground bounds it on the southwest, so that it presents the appearance of an old, broad, level-bottomed valley lying between this ridge on the west and southwest and the slopes of the Summit Upland on the east. This Sub-summit Plateau extends south as far as Toowa Valley, but in this direction it 1s much dissected by widely flaring, V-shaped canons of stream erosion. Glimpses of its flat top are obtained from the summit of the voleanie cone which sits on the divide between Voleano Creek and the South Fork of the Kern. Within these general limits the area of Sub-summit Plateau including its dissection is about 50 square miles. Its general altitude is about 11,500 feet. Other Plateau Remnants.—No other remnants of plateau sur- faces which could be definitely correlated with this Sub-summit Plateau were observed within the basin of the Upper Kern. But on the Great Western Divide and in the region to the west of the Upper Kern Basin, there are remnants of flat topped summits some of which are the undoubted correlatives of the Summit Upland, while others might with equal reason be correlated with the Sub-summit Plateau. The best instance of the Summit Upland on the west side of the basin is that afforded by Table Mountain (13,625 feet). This is clearly the remnant of a plateau which has been, and is being, reduced in area by the encroachment upon it of the steep cliffs which eneirele the mountain. Other high peaks to the south of Table Mountain show similar but less pronounced fiat tops. These resemble the summit of Mt. Whitney in character, except that the summit of Table Mountain is even more level. Their high altitude seems a fair warrant for regard- iug them as correlatives of the Summit Upland. Beyond the limits of the Upper Kern Basin the most notable flat topped summit is a high plateau which lies to the west of Farewell Gap and Mt. Vandever, between the East Fork of the 310 University of California. [Vou. 3. Kaweah at Mineral King and the head waters of Horse Creek. A fine view of this plateau is obtained from Sawtooth. (Plate 45.4.) Its altitude as found upon the Kaweah sheet of the U.S. Geological Survey is about 11,200 feet. Its northern front is deeply indented by a fine series of glacial cirques; and the topo- graphic map clearly indicates that cirques exist also on the south side. The summit surface is flatly undulating, and although upon the topographic map it appears merely as a high ridge, yet it has the expanse characteristic of the residuum of a plateau. The narrowness of the plateau is clearly due to the reduction of its area by the process of cirque encroachment from either side. This plateau may possibly be an outlying remnant of the Summit Upland, but owing to its lower altitude and to the fact that it abuts upon the steep, upper slope of Mt. Vande- ver, it seems better to suggest its correlation with the Sub- summit Plateau, with which, in these respects and in its general aspects, it is in better agreement. It may be well to remember here that, in recognizing and naming these two upland surfaces, we are not dealing with the hypsometrie congruence of mountain crests such as is too often relied upon for the identification of dissected peneplains. In the latter ease the peneplains are hypothetical. They may in some cases possibly have never existed. But there can be no possibie question as to the actual existence of both the Summit Upland and the Sub-summit Plateau. They are observable features of the geomorphy of the region. Hypotheses, of course, come into play the moment we begin to correlate isolated remains of old surfaces, but these, however frail, do not weaken the fact of the existence of these features or their importance in the historical eeology of the region. Sculpture of the High Mountain Zone.—The rugged mountains which girdle the Upper Kern Basin or rise within its area, and which have been placed in a geomorphic zone by themselves, the High Mountain Zone, owe their character to the sculpture of both upland and plateau. They are the remnants of a dissection of a lofty landmass which was, at one time in its history, limited upward by a surface in two general levels, that of the Summit Upland and that of the Sub-summit Plateau. Where sharp BUC DEP Ie GEOEMUINIV CAE VOL. 3, PE. 33, A remnant of the Summit Upland. Looking towards Mt. Whitney from Mt. Guyot. U-shaped glacial trough of Guyot Creek on the right. Jointed granite in foreground. Photo. by J. N. LeConte. Transitional slopes between Chagoopa Plateau and the south side of the Kaweah Ridge. Photo. by J. N. LeConte. Lawson. ] The Upper Kern Basin. 311 peaks and crests prevail these features are due to the intersection of opposing canon and cirque slopes below the level of this gen- eral surface, or to the intersection of such slopes with the steeper slopes of the Summit Upland. Inasmuch, however, as the upper limit of the second geomorphic, or High Valley, zone, the rear of the Chagoopa Plateau, approaches the level of the Sub-summit Plateau, by far the greater proportion of the High Mountain Zone is the result of the sculpture of the mass whose surface was the Summit Upland. 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ANDREW C. LAWSON, Editor A NEW CESTRACIONT SPINE FROM THE LOWER TRIASSIC OF IDAHO BY HERBERT M. Evans. CONTENTS. PAGE Occurrence and State of Preservation... cccceeee cececeeeeeee seeeeeeeveceeeeeeeees 397 ID NEVER ORO) 0 oak eee eee en ee ccc en nad eee 398 PANT MING OS 2 Oe eat cma aes feat Be igh Sele Sas a alae assets, ae wey OOD OCCURRENCE AND STATE OF PRESERVATION. The fossil fish spine described in the following paper was obtained on a palaeontological expedition to southern Idaho, during the summer of 1903, for the purpose of examining the lower Triassic exposures at Aspen Ridge and Paris Canyon. The spine was discovered at the latter loeality by Professor John C. Merriam, to whom the author is indebted for advice in the study otf the specimen. It was found in an exposure of the lower Triassic in Paris Canyon and about one mile west of the town of Paris. The associated invertebrate fauna was examined by Professor James Perrin Smith of Leland Stanford Jr. University, who was a member of the party. Professor Smith has made a special investigation of both the Aspen Ridge and the Paris beds, and the geologic position of the Paris horizon is best given in the following note which he has kindly furnished: “The beds in Paris Canyon are lower Triassic but below the typical Meekoceras beds of the Aspen range. They contain species of the genera Meehoceras, Prionolobus, Ophiceras, Pseu- 398 University of California. [Von. 3. dosageceras, and Celtites. The Pseudosageceras seems to be the only species common to these beds and those of the Aspen ridge.” On splitting the slab containing the specimen, the spine broke from the surrounding matrix leaving on the rock, the thin surface layer of the spine, together with the ganoine-coated tubercles which ornamented it. Consequently the ornamentation of the spine by tubercles was not at first evident. As tubercles were supposed to exist, the surface was carefully etched with hydrochloric acid and thus the whole pattern was brought out clearly. Numerous individual tubercles were then extracted and examined under the microscope. The figure of the spine (Pl. 47, Fig. 1) was based on a study of the complete tubercular pattern which was exhibited after the etching had exposed all of the tubercles present. The arrange- ment and ornamentation of the tubercles are given exactly as they occur on the specimen. Three transverse fractures of the spine permitted a study of the cross sections and furnished evidence of the character and extent of the medullary cavity (Pl. 47, Figs. la, 1b, le). The exact character of the deep posterior furrow at the base was brought out clearly by careful removal of the limestone matrix which filled it. (Fig. 1d). DESCRIPTION. Cosmacanthus elegans n. sp. PLATE 47. Type specimen No. M9087 University of California, Palaeontological Museum. Spine of medium size, 163 mm. long by 23 mm. greatest width, bilater- ally symmetrical, tapering, slightly arched, curving backward, cross-section triangular with a sub-acute anterior angle; anterior edge covered above the base by a rounded enamel ridge. The oblique dorsal line separates a smooth base from the ornamented exserted portion and indicates a posterior inclina- tion of about 45°. The lateral faces are slightly rounded. The posterior face is truncated and hollowed below by a deep furrow which is an extension of the medullary cavity. Upper portion of posterior face longitudinally elevated in a low, rounded, median ridge, or keel, between which and the edges of the face are shallow longitudinal furrows. The lateral and posterior faces are covered with small, closely set, and distinctly sculptured tubercles. The seulpturing of the tubercles is in the form of minute oblique lateral ridges which are generally longer on one side of the tubercle, thus making the pattern somewhat asymmetric; the obliquity of the ridges often approx- imates a spiral type. The sides of the tubercles curve sharply into a Evans.] A New Cestraciont Spine. 399 truncated top. On the upper third of the spine, the tubercles are disposed in longitudinal rows parallel with the anterior edge. They increase in number below and dispose themselves in perceptably oblique rows, tending to radiate from the central portion of the posterior edge. The medullary cavity extends for about .85 of the length of the spine and opens in a wide and deep furrow on the lower end of the posterior face. The edges of the lower end of the furrow are sharp and slightly incurved, becoming rounded as they approach each other above to meet near the upper end of the inserted portion. AFFINITIES. Isolated dermal spines closely resembling the above in many particulars occur at numerous horizons, being most common on this continent in the Devonian, Sub-Carboniferous, and the Coal Measures. They have been usually grouped under the general ’ term “Ichthyodorulites ” and are most frequently referred to the Cestraciontidae. Among the Iechthyodorulites, a great diversity of form and ornamentation exists, but many spines ean be found having some characters in common with the Paris specimen. The smooth base, ornamented faces, and the internal cavity with a low posterior opening, are characters possessed by many genera. Of the European genera, Asteracanthus Agassiz is near this spine in general form and ornamentation, but the similarity breaks down on examination of the individual tubercles and of the posterior surface. One of the conspicuous differences is seen in the entire absence of enlarged tubercles, denticles or teeth on this spine, whereas it possesses a sharply defined enamel keel, which is not present in Asteracanthus. The tendency to arrangement of the tubercles in transverse rows is a character perhaps most marked in Oracanthus Agassiz. This genus, however, never shows truncation of the posterior border and the tubercles are also distinetly different from those of the Paris spine. The general shape of the Paris specimen and its cross-sections, present a strong similarity to the figures of Memacanthus mont- lifer Agassiz* from the Triassic of England, but the presence of a well marked postero-lateral row of denticles as also the character of the lateral tuberculation in Nemacanthus preclude its refer- ence to that genus. * Agassiz L. Recherches sur les Poissons Fossiles. III Atlas 1843. Tab. 7, Figs. 11, 13, 14, 15. 400 University of California. [Von. 3. Some similarity also exists between this spine and the fragment from the Sub-Carboniferous which St. John and Worthen* have deseribed as Glymmatacanthus, but with such evidence as is at hand one would not be justified in establishing any certain affinities between the two. We know nothing of the character of the posterior face of Glymmatacanthus, which, moreover, shows no close agreement in the seulpturing or arrangement of its tubercles and possesses no anterior keel. The Paris spine ean be ineluded in the genus Cosmacanthus Agassiz as defined by Woodward.t Its general form, the pres- ence of tuberculation on the lateral faces, and the truneation of the posterior face with low longitudinal keel, are characters which show its relationship to that genus. Of the species which have been included in Cosmacanthus, the Paris specimen shows closest affinity with two which St. John and Worthen have deseribed from the Sub-Carboniferous of Illinois and Missouri, and of these, especially with Cosmacanthus (Geisacanthus) stellatus. This spine shows clearly the prominent anterior enamel keel, a character which was apparently absent in the type species, C. malcolmsoni Agassiz from the old Red Sandstone, as well as in C. marginalis Davis and C. carbonarius MeCoy, from the Irish Carboniferous. It may well be questioned whether this character is not of generic rank and if so the name Geisacanthus must be retained for the keeled forms. The Paris spine is easily separated from the Illinois species by its much greater size, more numerous tubercles and different tubercular pattern, as well as by the difference in the form and sculpturing of the tubercles. For the present we retain it as an Ichthyodorulite, until further information such as its association with teeth, scales, ete. will permit us to identify it with some other form or certainly fix its generic relationship. At the present time, this is, so far as the author is aware, the only Ichthyodorulite recorded from the American Triassic. *St. John O. and Worthen A. H. Descriptions of Fossil Fishes, Palaeontology of Illinois. Geol. Sury. of Ill. (A. H. Worthen, Director) 1875. Vol. VI, Part II, pp. 446-447; also pp. 440-442. + Woodward, A. S. Catalogue of the Fossil Fishes in the British Museum. Part II, 1891, p. 111. EVANS. A New Cestraciont Spine. 40] It is interesting to note that oceurring in the lower Triassic, its affinities are so close with some of the Carboniferous species. Probably a better knowledge of the iehthyie fauna of our early Triassie will attend a further study of the Idaho beds. University of California, May, 1904. EXPLANATION OF PLATE 47. Cosmacanthus elegans n. sp. Fig. 1.—Lateral view of spine. (Natural size). Figs. la, 1b, le. —Cross sections of spine taken at a, b, c, on figure 1, show- ing form and extent of the medullary cavity. (Natural size). Fig. 1d.—Posterior view of base of spine showing character of deep medul- lary furrow. (Natural size). Fig. 2.—Top view of a tubercle showing typical form and sculpturing Cee air Fig. 2a.—Lateral view of the tubercle shown in figure 2. (> 12.5). Vi@ Er Sie rlen e7, BULLE DEPIn GEOL UNIV, CAE. Se _ UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology eS as. es Vol. 3, No. 19, pp. 403-410, Pls. 48-49. ANDREW C. LAWSON, Editor — ae. A FOSSIL EGG tS ae ; ' FROM Agee ae ARIZONA ! ae : . BY WM. CONGER MORGAN neat AND 2 ey MARION CLOVER TALLMON . A Sn Pei sf as os SIQAG ; | l A804 f WZ LA =F ZI OCIS” * a Nyy a Se TZED pv os ANT7 vannese=enanang, eee, IZED, se _ BERKELEY Ree he fs THE UNIVERSITY PRESS t JUNE, 1904 PRICE 10 CENTS may be purchased at the following prices from the University Librarian ie - Rowe No. 10. Mineralogical Notes, by Arthur S. Hakle 2 el No. 11. Contributions to the Mineralogy of California, by Walter C Blasdale | No. 12. The Berkeley Hills. A Detail of Coast Range Geology, og: Andrew | Tei is designed to have these made up into volumes of froin 400 to 500 page per volume is placed at $3. 5°, including postage. The papers composing the ai whom remittances should be addressed:— Bee: a - VOLUME 1. Se ev ee ae : NOs. Te bhe Geology of Carmelo Bay, by Andrew C. Lawson, with chemical a ses and coéperation in the field, by Juan de la C. Posada aes No. 2. The Soda-Rhyolite North of Berkeley, by Charles Paltiche - ‘s No. 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome —_ ; No. 4. The Post-Pliocene Diastrophism of the Coast of Southern California, : Andrew C. Lawson : ioe Price, No. 5. The Lherzolite-Serpentine and Associated Rocks = the Potreo, San- Vr oie Francisco, by Charles Palache — ogee No. 6. Ona Rock, from the Vicinity of Berkeley, icon eintae a New Soda 3 ree ; Amphibole, by Charles Palache ~~. on No. »7. The Geology of Angel Island, by F. Leslie Ransome, ‘with a Note on the | >, ~ Radiolarian Chert from Angel Island and from Buri-buri Ridge, San — ; Mateo County, California, by George Jennings Hinde . . Price, 4 No:= 8) athe Geomorphogeny of the Coast of Northern California, by Andrew C. — x ; Lawson E Price, < No. 9. On Analcite Diabase from San Luis ‘Obispo County, ‘California, by Harold W. Fairbanks No. 10. On Lawsonite, a New Rock- forming Mineral from the baron Penins la, Marin County, California, by F. Leslie Ransome, . ie Re No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte. Pric 12. On Malignite, a Family of Basic, Plutonic, Orthoclase Rocks, Rich in Alk % A lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, é : by Andrew C. Lawson 3 Price, 250: ' No. 13. Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene, Heat am. + Berkeley, by John C. Merriam : ef Price, Ioc No. 14. The Great Valley of California, a Criticism of te. © Theory of Heaven by : : #B Leslie Ransome . . Ae: eytieas acces, Ys Paice, 5. VOLUME. Ws < x SNo: “i: The Geology of Point Sal, By Harold W. Fairbanks © See No. 2. On Some Pliocene Ostracoda from near Berkeley, by Frederick Cha man . Ne rile No. 3. Note on Two Tertiary Faunas from the Rocks of the ‘Southern Coast Vancouver Island, by J.C. Merriam . Pri No. 4. The Distribution of the Neocene Sea-urchins a Middle ‘California, face Bearing on the Classification of the Neocene ‘ormations, Py: Job Merriam : a= é No. 5. The Geology of Point Reyes Peninsula, by F. M. Anderson o x No. 6. Some Aspects of Erosion in Relation to the Theory of the Peneplain, by W. | : S. Tangier Smith _ Price, 2 No. 7. A Topographic Study of ‘the Islands of Southern ‘California, by Si - Tangier Smith : 5 No. 8, The Geology of the Central Portion of ‘the Isthmus of Panama; bye Hershey c No. 9. A Contibutiea to the Geology of the Jobn Day Basin, by John son and Charles Palache UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 19, pp. 403=410, Pls. 48-49. ANDREW C. LAWSON, Editor A FOSSIL EGG FROM ARIZONA. BY Wm. CoNGER MORGAN AND MARION CLOVER TALLMON. CONTENTS. PAGE Tatts X@Ya ERC ao ate ee eee nee SR Pane NO eR OD 403 (ONCE ADRENALS) or eee sR al a 404 The Enclosing Capsule.................. eee ey ea ey eee ee eee 404 AIpvOmPH TO OM S16) 4 Bae eae ies as «aoe © reese sys scyee coca cic geece Gealeecs ee Sen eee 405 The Contents .......... a ame ae ee oe ese 406 TNS eNO GY HS eR I Rr Se eC 409 INTRODUCTION. Very few instances of the occurrence of eggs in the fossil state have been recorded. The fossil eggs of New Zealand birds are shells which have been preserved by reason of their thickness and strength. The Chelonian eggs of Tertiary age from Auvergne, France, are simply shells filled with hardened mud. An interesting fossil egg from the American Miocene has been deseribed by Oliver C. Farrington and has been considered the ege of a duck. The specimen described in this paper was brought to the attention of Professor John C. Merriam some months ago by Mr. G. A. Helmore of San Francisco. It had been in Mr. Helmore’s possession for some years and was obtained by him from a pros- pector who had found it in a large pebble embedded in placer * Field Columbian Museum, Pub. 35. Vol. [, No. 5, Geol. Series. A Fossil Egg from South Dakota. 404 University of California. [Vor. 3. gravels on the Gila River in Arizona. Mr. Helmore being unwilling to part with the specimen has kindly loaned it to the University for study and deseription. When found, the egg formed the center of a rounded mass of hard caleareous rock which may be ealled the capsule. The surrounding matrix had been, partly removed and the egg broken open before it came into our possession. As it was necessary to obtain a fresh unrubbed surface of the shell for study, the enclosing rock was removed in the laboratory. Since this seems to be a unique specimen it has been thought advisable to put the principal facts concerning its preservation on record. The authors are indebted to Professor Merriam for many suggestions during the course of this study. OCCURRENCE. Unfortunately, the information which we have concerning the occurrence of this specimen does not give us very definite evi- dence concerning its age. The eneapsuled egg is said to have been a pebble in gravels some distance above the present level of the river. If, as has been supposed, the gravels are bench deposits, the eve is at least as old as the Quaternary. If they are of Recent origin we can still hardly suppose it younger than (Quaternary, as it is only under the most extraordinary cireum- stance that deposits of Recent origin can occur as hard pebbles in Recent conglomerates. THE ENCLOSING CAPSULE. The nature of the capsule when the specimen was first exam- ined is shown in Plate 48, figures 2 and 4. Some of the matrix had been removed at that time. The enclosing rock forms a flattened ellipsoid measuring about 3445 inches. The surface was sharply ridged, due apparently to differential weathering of the thin layers of matrix. The greater part of the matrix is highly caleareous and might be designated as Lmestone. The outer layer is of finely laminated clay. When the capsule was removed its inner surface was seen to be marked with peculiar pits (Pl. 48, figs. 83 and 4), and to be covered with a very thin film of a tarry material, which usually MorGAN-TALLMON. | A Vossil Hgg from Arizona. 405 fills the pits completely. The number of pits in any piece of the matrix corresponds in general with the number of visible pores in that part of the shell from which it was removed. (PI. 48, fig. 1.) These pores in the shell are also filled with tar, and the relative distribution of pits and pores over corresponding surfaces of matrix and shell is the same. Opposite a fine crack in the shell the quantity of tarry material is considerably increased. Chemical examination failed to show the presence of any tar in the matrix except this small quantity on or near the surface in contaet with the shell. THE EGG SHELL. The eee shell has retained its original composition and micro- seopie structure. A chemical analysis shows that it does not differ from the shell of a wild goose ege. A thin section (Pl. 49, fig. 2a) shows the same structure as that exhibited by a similar section from a hen’s ege. The form of the eve has been perfectly preserved, and from comparison with existing eges we conclude that this specimen belonged to an aquatic bird. The egg corresponds fairly well to the type of egg laid by the cormorant. Objection might be made that the cormorant’s ege is covered with a chalky layer, but when this layer is removed a pitted surface much like that of this specimen is exposed. The minutest markings of the shell are preserved in the matrix, and in this there is no evidence of any seratches such as usually occur in the chalky layer of the cormorant’s egg. It seems improbable that the chalky layer would have been washed off without injury beine done to the ege, neither is it probable that it was firmly united with the matrix and pulled away in separating the egg shell from the rock. While the specimen much resembles the type egg of the cormorant, it is also very much like the egg of the larger grebes or herons, the American bittern and the limkin. Again, while the ratio of the short to the long axis is somewhat less than that of the typical egg of a duck, it corresponds almost exactly with measured eggs of many of the larger species of this family. It is probable that when this egg was deposited the region was not near to the sea. Under geographic conditions 406 University of California. [Vou. 3. sunilar to those now obtaining dueks would be much more numerous than any of the other possible forms, and the proba- bilities, therefore, favor its anatine origin. Considering that great individual variation often occurs in a single set of eggs, it is evident that specifie conclusions as to the parentage of any specimen can hardly be drawn from form alone. THE CONTENTS. With the exception of a small space near the periphery, the interior of the egg is filled solidly with a beautifully crystalline mass of the mineral colemanite (Pl. 49, fig. 1). In several places next the shell there is present a dark brown semi-fluid tarry inaterial (PI. 49, fig. 1,4) resembling asphalt in appearance and physical properties. When cold it is brittle, showing a conchoidal fracture with brilliant surfaces, the edges of the fracture becoming rounded on standing. As the temperature rises it grows softer, until at 100°C it becomes a fluid with considerable viscosity. Its specific gravity is a trifle less than that of boiling water. It is readily and completely soluble in petroleum ether, carbon disulphide and chloroform. Henee it resembles very closely that fraction of natural asphalts which has “ petrolene.” been known as Between 150° and 250°C a far-reaching decomposition takes place, resulting in the liberation of relatively large volumes of an inflammable gas. Of the residuum in the ignition tube after such treatment, about fifty per cent only is soluble in petroleum ether. The greater part of the remainder dissolves in carbon disulphide, but an appreciable residue is soluble only in chloro- form. It is thus evident that the substance obtained after heating cannot be differentiated from a natural asphalt, since it may be separated into the so-called “asphaltene,” as well as the “petrolene” fraction, by the ordinary methods. Submitted to ultimate analysis the same similarity is apparent. Qualitatively examined the tar shows the presence of carbon, hydrogen and sulphur, but not of nitrogen, and although, as it oceurs In the egg, the tar contains apparently a smaller percent- age of carbon than is found in asphalts generally, the heated MorGANn-TALLMON, | A Fossil Egg from Arizona, 407 material contains the normal constituents in the normal propor- tions, These facts tell us something of the history of the fossil during the period in which it lay buried, and also show the rela- tion of the tar it contains to other bituminous matter. Since the tar is completely soluble in petroleum ether without residue of any kind, while the heated product is largely insoluble in the same menstruum, it is evident that the fossil has never been subjected to a temperature as high as 150°C. The tar as it exists in the evg@ requires simply this sheht elevation of temper- ature to make it indistinguishable from a natural asphalt. While the colemanite is often in direct contact with the shell, the bituminous material is always so. 227 Cireumference (longitudinally) 0.000... eee cree 169 22 (transversely) ....... BE hh OnE Sees ane 124 Long diameter of enclosing capsule 2... eee eee eee 120 Average thickness of enclosing capsule ......00.00.02 eee ee eee eee 12 Thickness of cog'ovshh ell. oe eects ee ere econ devon se aaesuendh, axsniemseaes 03 —— = EXPLANATION OF PLATE 48. A Fossil Egg from Arizona. All figures natural size. Fig. 1.—Side view. Fig. 2.—Egg in the original matrix. Fig. 3.—Matrix from inner side, showing pits. Fig. 4.—In the matrix, end view. BULREY DEPT. GEOL) UNIV. GAL, VOlens, Play 48) ’ i 1 \ - oot ‘ a Fig Fig. Fig. EXPLANATION OF PLATE 49. A Fossil Egg from Arizona. . 1.—Fractured surface of the broken egg, showing the contents; t, t’ and other darkened areas represent the bituminous material; the remainder of the cavity is filled with colemanite. (Natural size.) @. 2a.—A portion of the egg shell ground down on one side. 8, corru- gated outer surface; ¢c, cellular lower layer. (* 275) ig. 2b.—Cross-section of the shell fragment shown in figure 2a. s, corru- o gated outer surface; ¢, cellular lower layer. (% 275) 3.—Outer surface of the shell, showing corrugations of the surface and a large pit filled with bituminous material. (* 275) 4.—Cross-section of the pit shown in figure 8. (* 275) BULL. DEPT. GEOL. UNIV. CAL. VOER 3 Rika? baie us Thats AO ‘ ay hs ve ui 4 = 4 wa oes +3 it * &: eu Z eet) % Pe 5" his mit? Pe 9 Ls af ‘ a a UNIVERSITY OF CALIFORNIA PUBLICATIONS -. Bulletin of the Department of Geology © “Vol. 3, No. 20, pp. 411-418, Pls. 50-51. ANDREW 'C. LAWSON, Editor ' EUCERATHERIUM, A NEW UNGULATE Sees _ FROM THE - QUATERNARY CAVES OF CALIFORNIA BY WILLIAM J. SINCLAIR AND y E. L. FURLONG 2 oS bs: soo’ io = SSS BERKELEY | THE UNIVERSITY PRESS JUNE, 1904 | ee 3 . PRICE 10 CENTS a hid | Ze eos lns¢y es ae 2 Vids, t-+8 ie 5 ~ \ WV ms Vops = Sonal Museu Z. } THE. BULLETIN OF THE DEPARTMENT OF GEOLOGY OF THE UNIVERSITY OF CALE FORNIA is issued at irregular intervals in the form of separate papers or memoirs, each - ‘embodying the results of research by some competent investigator in geological science. “It is,designed to have these made up into volumes of from~4o0 to 500 pages. The price — per volume is placed at $3.50, including postage. The papers composing the Volumes will be sent to subscribers in separate covers as soon as issued. The separate numbers may be purchased at the following prices from the University Librarian, J. C. Rowell,to whom remittances should be addressed:— VOLUME 1. F No. 1. The Geology of Carmelo Bay, by Andrew C. Lawson, with chemical analy- ses and cooperation jn the field, by Juan de la C. Posada : Price, 25¢ : No. 2. The Soda-Rhyolite North of Berkeley, by Charles Palache S| Price=T0C mms No. 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome Price; 4oc No. 4. The Post-Plidcene Diastrophism of "the Coast of Southern California, by - Andrew C. Lawson 2 i Price, 4oc No. 5. The Lherzolite-Serpentine-and Associated Rocké of the Potreo, Sal eed Francisco, by Charles Palache enter? No. 6. Ona Rock, from the Vicinity of Berkeley, ‘containing a New Soda Price, 30¢ ~ Amphibole, by Charles Palache : No. 7. The Geology of Angel Island, by F. Leslie Ransome, with a Note on, the Radiolarian Chert from Angel Island and from Buri-buri Ridge, San Mateo County, California, by George Jennings Hinde Sls hase’ BRIGG wage No. 8. The Geomorphogeny of the Coast of Northern California, by Andrew C. , Lawson 5 Price, 30c No. 9g. On Analcite Diabase from San Luis Obispo County, California, by Harold W. Fairbanks_ . ; >. Priee, 25¢ No. 10. On Lawsonite,.a New Rockagrating Mitieral from the Tiburon Peninsula, Marin County, California, by F. Leslie Ransome . : Price, roc No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte. Price, 20c No. 12. On Malignite, a Family of Basic, Plutonic,-Orthoclase Rocks, Rich in Alka- lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, by Andrew Lawson : Price, 20c No. 1 3. Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene, near Berkeley, by John C. Merriam. : Price, roc No. 14. The Great Valley of, California, a Criticism of the Theory of Isostasy, by F. Leslie Ransome ; ; 5 : Price, 45¢ VOLUME 2. No. 1. The Geology of Point Sal, By Harold W. Fairbanks . Price, 65¢ No. ~2. On Some. Pliocene Ostracoda from near Berkeley, by Frederiek Chap-— man . Price, Icc No. 3. Note on Two Tertiary Faunas from the Rocks of the Southern Coast of Vancouver Island, by-J. C. Merriam > . Price, oc No. 4. The Distribution of the Neocene Séa- urchins of Middle "California, ‘and Its Bearing on the Classification of the Neocene Formations, by John C. Merriam i ‘ : Price, toc No. 5, The Geology of Point Reyes Peninsula, by F. M.‘Anderson = . Price, 25¢ No. 6. Some Aspects of Erosion in Relation to the Theory of the Peneplain, by W. S. Tangier Smith : ? Price, 20¢ No. 7. A Topographic Study of the ‘Islands. of Southern California, by W. S. Tangier Smith Price, 4oc No. 8. The Geology of the Central Portion of ‘the Isthmus of Panama, by Oscar H. : Hershey : ‘ Price, 30¢ No. 9. A Cohenoution to the Geology of the Tata Day Basin, by John C. Merriam Price, 35¢ No. 10, Mineralogical Notes, by Arthur S. Kakle - : Price, Ioc No. 11. Contributions to the Mineralogy of California, by Walter C. Blasdale Price, 15c — No. 12. The Berkeley Hills. A Detail of Coast Range Geology, By Andrew C. Law- — son and Charles Palache . tar - E 0 . Price, 0c UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 20, pp. 411=418, Pls. 50-51. ANDREW C. LAWSON, Editor EUCERATHERIUM, A NEW UNGULATE FROM THE QUATERNARY CAVES OF CALIFORNIA. BY WILLIAM J. SINCLAIR AND E. L. FURLONG. CONTENTS. PAGE Tira GIO CU CUT OM eee psectt sccsee ccelecsczseececetstesccesasticeices TOE NT eA PEE ERROR PR REET 411 Euceratherium collinum Furlong & Sinclair... ccc cee eee ee 412 GeMeT] CRCMALACTOLS fers areca eens eras, o8e ccs eee eeeeee ec sees ceesvanibstceciges eee 412 SDECTIIGRCNATLACTOL Shae tees caverta, streets coiseet: ccsncstveves sae caoesecsyethtieardec1 sevsetsvesri2 412 CCT ET. COM eet sine. et nee, cue tee eran eee tes hs cee fo Beat eae oa site eee ccaaese 412 (CHRD Wa ey gy Re AR or Dentition : PANETT GCS pete eres eae eee een eae es te See ase 2A eect rea ioe ee 28 Soe) 416 WML @ENEACERED GOVE eH SIE eg Oa oh ee eye eee aS 417 INTRODUCTION. While conducting explorations in the Quaternary caves of Shasta County for the Department of Anthropology of the Uni versity of California, the writers have frequently found portions of the skeleton of a large ungulate differing in many respects from any existing form. The discovery by Mr. Furlong, during the past summer, of the exceptionally complete specimen described in the present paper, made possible the reference of this more or less scattered material to a new and peculiar genus, for which the name Euceratherium' has been proposed.” 1 Evxépaos, beautiful-horned; @nplov, wild beast. 2 Pub. Univ. of Cal. Am. Arch. and Eth. Vol. 2, p. 18. 412 University of California. [Vou. 3. EUCERATHERIUM COLLINUM Furlong & Sinelair. Pus. 50 and 51; Text Fia. 1. Pub. Univ. of Cal. Am. Arch. and Eth. Vol. 2, p. 18. Generic characters.—Horn-cores solid, situated close together on the posterior extremity of the frontals and far behind the orbits. Frontals reaching to occiput, with strongly developed pneumatic eavities extending into the bases of the horn-cores. Parietal confined to occiput, forming no part of the cranial roof. Lachrymal pit broad and shallow. Dental formula ©, 9, 3, 3. Teeth hypsodont, large, without cement or accessory cuspules. Specific characters.—Horn-cores laterally compressed and curved, elliptical in cross-section at the base, circular in cross- section at the tip. Proximal half of horn-core directed upward and backward, distal half outward and forward. Frontals broadly convex above orbits, shghtly inflated toward bases of horn-cores. Occiput with sharp median keel above foramen magnum. Occurrence.—The type specimen (No. M8751, Univ. of Cal. Palaeont. Mus.) was discovered by Mr. Furlong in the Samwel Cave, situated on the east side of the McCloud River, about thirteen miles north of Baird, Shasta County, and 355 feet above the river. It consists of a cranium without mandible, from which a part of the right horn-core, the jugal process of the right squamosal, and the extremities of the premaxillae and nasals have been broken. The nasals and a part of the pre- maxillae have been restored in plaster. The superior dentition lacks only the first premolar on the left side. The eranium lay on the surface of a deposit of ossiferous clay flooring a deep vault in the cave, and was almost completely covered by a coat- ing of crystalline stalagmite. The difficulty of preparing the specimen for exhibition was increased by the chalky character and extreme thinness of the bones of the skull, especially in the frontal region where the pneumatic cavities are roofed over by mere shells of bone. In the Potter Creek Cave, Huceratherium is represented by abundant remains which have been found in all the bone-yield- Sincuarr-Furtona.] Huceratherium, A New Ungulate. 413 ing strata. This material comprises broken horn-cores, teeth and podial elements. The horn-cores and teeth agree closely with those of the type specimen. The age of the deposit in the Samwel and Potter Creek Caves is later Quaternary, but the Potter Creek Cave is probably the older. Cranium.—The eranium is that of a fully matured individual In size it approximates the skull of a small cow, and resembles Bos in the elongated facial region and the restriction of the parietal to the oeciput. In the front view (Pl. 51), the facial region appears broad, in striking contrast with the narrowing of the forehead posteriorly. The interorbital area is broadly con- vex, becoming’ slightly inflated toward the bases of the horn- cores, as seen in the lateral view (Pl. 50), where the pneumatic cavities approach the surface, reducing the thickness of the frontals to a mere shell. The prominent orbits are well in advanee of the horn-cores. Opposite the posterior rim of each orbit there is a small supraorbital foramen. The frontals reach the oeeciput, exeluding the parietal from the cranial roof, and confining that element to the back of the skull. The horn-cores are supported by the frontals at the posterior extremity of the skull. Although situated close together, their bases do not coalesce. Internally, the cores are filled with can- cellous bone tissue and are not penetrated beyond their bases by the pneumatic cavities of the forehead. Proximaliy, the horn- cores are elliptical in cross section but become ecireular toward the tips. The proximal portions of the cores are directed back- ward and upward. Distally, they curve outward and forward with a slight upward turn toward the tip. They are pierced by many nutrient foramina and are deeply marked on the outer side by vascular channels. The anterior margin of the left horn-core bears two low prominences situated about half way up the shaft. These were not observed on any of the horn-cores from the Potter Creek Cave. On the back of the skull the parietal and occipital elements are fused into a vertical plate, which meets the frontal plane at an acute angle. Superiorly the occiput is narrow corresponding with the great narrowness of the forehead. It widens toward 414 Iniversity of California. (Von. 3. the middle, supporting a median tubercle for muscular attach- ment. The tubercle unites inferiorly with a sharp median keel which becomes less prominent toward the superior border of the foramen magnum. Lateral ridges extend from the median tuber- cle outward and downward over the mastoid as in the sheep. The base of the skull resembles that of Haplocerus, and the foramina for the exit of the eranial nerves are the same in char- acter and position as in that genus. The bullae are imperfectly preserved in the type, but in another specimen (No. M8464) from the Potter Creek Cave they are seen to be quite different from the corresponding: parts in existing North American ecavicorns. Instead of being high and narrow as in the cattle and sheep, they are flattened, presenting inferiorly a slightly concave surface with diamond-shaped outline. Anteriorly and externally, the bound- aries of this surface are sharply defined; posteriorly and inter- nally they are less clear. The bullae are low, extending but a short distance (6 mm.) below the level of the post-glenoid pro- cess. In Ovibos, the rugged bullae present a mammilated erest inferiorly, quite different from the flattened surface in Hucera- theriune. The free borders of the palatines at the anterior margin of the posterior nares are pinched in a short distance below the narial border, producing on either side a shallow fossa which is not found in any of the North American cavicorns with which this genus has been compared. The contour of the dental series is the same as in Ovis and Hapilocerus, and as in these forms the posterior palatine foramina open on the maxillo-palatine suture. In the lateral aspect of the cranium (Pl. 50) the superior border of the temporal fossa is seen to be sharply limited by a ridge which extends from the upper margin of the postorbital bar beneath the base of the horn-core to the lateral border of the occiput which bounds the fossa posteriorly. The malar areh is robust. That portion of it which is included between the inferior orbital rim and the ridge which extends backward as the lower border of the jugal process is broader than in the domestic eattle. The lachrymal pit is a broad shallow coneavity, limited above Sinciair-Furtona.) Huceratherium, a New Ungulate. 415 by a low ridge along the line of the fronto-lachrymal suture. Anteriorly and inferiorly the boundaries of the fossa are indefinite. The maxillary is considerably inflated some distance above the alveolar border, giving to the face a swollen appearance. The anterior opening of the infraorbital canal on the left side is double and is situated above the anterior margin of the fourth premolar, the smaller foramen opening above the larger one. On the right side, the opening of the canal is single. Dentition.—The dentition resembles closely that of Ovibos, but the length of the superior series is somewhat shorter than in that genus. The teeth are hypsodont, without trace of cement or accessory cuspules. The second premolar on the left side is wanting, and the third is abnormally inserted with its outer wall in contact with the anterior margin of the fourth. In the occlusal view (Fig. 1) the premolars of the opposite side have been drawn. Fig. 1. Huceratherium collinum. Left superior dental series, >< +. The pattern of P? has been obscured by wear. The wall of the inner crescent of P® is interrupted by a sharp angulation, while that of the fourth presents the usual lunate outline. The teeth possess the typical selenodont structure characterizing the Ovinae. The external styles are prominently developed, bound- ing depressed areas with broadly convex median ribs. The lakes are narrow, and owing to the absence of cement remain open even in well worn teeth. The molars display the deep pit pro- duced by the confluence of the walls of the inner crescents which is characteristic of Haplocerus and the sheep. Superior incisors and canines were undoubtedly absent. 416 University of California. [Von. 3. As the teeth wear, those of the superior series increase in transverse diameter and decrease anteroposteriorly. This is due to the great obliquity of the inner erescents which slope from the triturating surface toward the palate, and to the anterposterior constriction of the long tooth crowns as the roots are approached. In the last superior molar, the anterposterior diameter remains more constant than in the other teeth, due to the posterior prolongation of the metastyle which tends to increase in width toward the alveolar margin. Affinities.—The closer affinities of Pucerathertum are not clear. It may be placed in the sub-family Ovinae but can not be regarded as intimately related to any existing North Ameri- can member of that group. The cranium is larger than in the bighorn sheep while the horn-cores are smaller, are situated much farther behind the orbits, and differ greatly in form and curvature. Although there is a resemblance to Ovibos in dental structure, the horn-cores are of entirely different type. Price wesc No. 10. On Lawsonite, a New Rock- forming Mineral from the Tiburon Peninsula, Marin County, California, by F. Leslie Ransome . 4 Price, Ioc No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte. Price, 20c No. 12. On Malignite, a Family of Basic, Plutonic, ‘Orthoclase Rocks, Rich in Alka- lies and Lime, Intrusive in the Cout¢hiching Schists of Poohbah Lake, by Andrew C. Lawson 5 eo Priceyzow No. 13. Sigmogomphius Le .Contei, a New Castoroid Rodent, from the Pliocene, near Berkeley, by John C. Merriam. 3 Price, roc No. 14. The Great Valley of Saag a Criticism of the Theory of Isostasy, by F. Leslie Ransome . : . ; Price, 45¢ VOLUME 2: No. 1. The Geology of Point Sal, By Harold W. Fairbanks .. sPrices65e5 No. 2. On Some Pliocene Ostracoda from near Berkeley, by Frederick Chap- man. Price, Icc No. 3. Note on Two Tertiary Faunas from the Rocks of the Southern Coast of Vancouver Island, by J.C. Merriam . . Price, Ioc No. 4. The Distribution of the Neocene Sea-urchins of Middle ‘California, and Its Bearing on the Classification of the Neocene Formations, by John C. Merriam . 4 5 Price, Ioc No. 5. The Geology of Point Reyes Peninsula, by F.M. Anderson +. Price, 25¢ No. 6. Some Aspects of Erosion in Relation to the Theory of the Peneplain, by W. S.. Tangier Smith ‘ . Price, 20c 7 No. 7548 Topographic Study of the Islands of Southern California, by W. S. (eee Tangier Smith 2 Price, 4oc 13 No. 8. The Geology of the Central Portion of the Isthmus of Panama, by Oscar H. Hershey : -. ZSP rice 20 No. 9. A. Sontabaied to the Geology of the John Day Basin, by John C. Merriam Price, 35c No. 10. Mineralogical Notes, by Arthur S. Hakle : 3 Price, 0c | No. 11. Contributions to the Mineralogy of California, by Walfer C. Blasdale Price, 15¢c No. 12. The Berkeley Hills. A Detail of Coast Range ’ Geology, by Ang Cc. Law- ; son and Charles Palache : saad 5 : 3 : Price, Soares UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 21, pp. 419=421. ANDREW C. LAWSON, Editor A NEW MARINE REPTILE FROM THE TRIASSIC OF CALIFORNIA BY JOHN C. MERRIAM. In the collections of marine Triassic reptiles at the University of California there are a number of specimens representing a heretofore unknown form of swimming: reptile. In advance of a more complete discussion of the structure and affinities of this group, the following description of the type specimen is presented. Thalattosaurus alexandrae, new gen. & sp. FIGURE 1. Cranium elongated, with slender snout. External nares separated and not far in front of the orbits. Dentigerous portion of the premaxillaries elongated but shorter than the maxillaries. Premaxillaries and maxillaries seulptured on the external surface. Vomers with two rows of flat, button-like teeth. Pterygoids with four or more rows of curved, conical teeth. Palatines not known to be dentigerous. Teeth of the premaxillaries and of the anterior end of dentary slender conical. Posterior part of dentary and. probably of maxillaries with button-like, flat or only slightly tubereulate teeth. Vertebrae amphicoelous, neural spines slender. Dorsal ribs single-headed. Coracoid reniform, elongated antero-posteriorly. Seapula narrow. Humerus short, much expanded distally. Radius and ulna about half the length of the humerus; radius with median constriction. Pelvie arch robust, inferior elements not plate-like. 420 University of California. (Vou. 3. The type specimen (No. $343 Pal. Mus. Univ. Cal.) was found im the Trachyceras beds of the Hosselkus limestone in the Upper Triassic of Shasta County. It ineludes the anterior two- thirds of the skull and a portion of the temporal region; also parts of over thirty vertebrae, numerous fragmentary ribs, the principal elements of the pectoral and pelvic arches and a considerable portion of an anterior limb. Fig. 1. Thalattosawvus alevandrac. Inferior side of the anterior portion of the cranium. M, maxillary; Pm, premaxillary; V, vomer; Pl, palatine; J, jugal; N, narial opening. ™ 4. This species is named in honor of Miss A. M. Alexander, who has not only contributed generously to the financial support of the work on the vertebrates of the marine Triassic but was herself the discoverer of the type specimen furnishing: the largest part of our information concerning the group: In its fundamental outlines, the skeletal structure in Thalatto- saurus is strongly suggestive of the Rhynchocephalia, but like many of the so-called rhynchocephahan groups it differs so far from the typical forms represented by Sphenodon, Homae- osaurus, ete., that it can not be included in the same ordinal division. it is likewise so different from all of the other described reptilian families and orders that it must be given an independent position. The family name Thalattosauridae and the ordinal: name Thalattosauria are therefore used to express its position in the scheme of classification. — Recently a number of groups possessing rhynchocephalian characters have been tentatively brought together as orders in a superorder, Diaptosauria, by Osborn.* Although diaptosaurian in one sense simply spells primitive, this classification serves to emphasize the distinct kinship certainly shown by many of these *H. F. Osborn. The Reptilian Subclasses Diapsida and Synapsida and the Early History of the Diaptosauria. Mem. Am. Mus. Nat. Hist., Vol. 1, Part 8, 19038. Merriam] A New Marine Reptile. 421 forms. For the present the Thalattosauria may be placed in the superorder Diaptosauria, though it is doubtful whether it will be retained in that division or even whether the Diaptosauria can hold together when the various forms included in it become better known. With increased knowledge of the Triassic reptiles, it will naturally become increasingly difficult to determine whether or not some of the orders classed with the Diaptosauria ave more deserving of a position in that group than, for example, the rhynehoeephaloid Parasuchia having’ an independent position. Inside the Diaptosauria the closest affinities of the Thalatto- sauria are with the Proganosauria and Choristodera. From both groups they differ more widely than these two differ from each other. In many respects, particularly in limb structure, the Thalattosauria represent more highly specialized aquatic forms than the other two orders. Outside of the Diaptosauria there are noticable resemblances to the Parasuchia and to the Lacertihans. The common char- acters are, however, almost without exception, primitive or rhynehocephalian characters which we find persisting in the Parasuchia and Squamata. *» Some of the most interesting points of resemblance to known forms shown by Thalattosaurus are found in its similarity in parts of the skull to Proterosuchus Broom, from the Karoo Beds. This form is referred to by Broom as “ a primi- tive Rhynehocephahan which shows a considerable degree of specialization along the line which gave rise to the early Croco- diles and Dinosaurs.” Here as in other groups compared, the skull structure shows important differences. Judgine’ from these differences and from the occurrence of Proterosuchus, we may expect that the limbs in that form will prove to have a structure very different from that in Thalattosaurus, and will tend rather toward the crocodilian type. While showing note- worthy affinities, it would be impossible to brine Proterosuchus and Thalattosaurus nearer to each other than related orders of the Diaptosauria could come. eae Ss a UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology ANDREW C. LAWSON, Editor Vol. 3, No. 22, pp. 423=475- THE RIVER TERRACES OF THE ORLEANS BASIN, CALIFORNIA BY OSCAR H. HERSHEY os Meta o Yo Y) F "te, oD s sag eo : \ BERKELEY L. THE UNIVERSITY PRESS NOVEMBER, 1904 PRICE 35 CENTS ae / THE BULLETIN OF THE DEPARTMENT OF GEOLOGY OF THE UNIVERSITY OF CALI: FORNIA is issued at irregular intervals in the form of separate papers or memoirs, each embodying the results of research by some competent investigator in geological science. It is designed to have these made up into volumes of from 400 to 500 pages. ‘The price per volume is placed at $3.50, including postage. The papers composing the volumes will be sent to subscribers in separate covers as soon as issued. The separate numbers may be purchased at the following prices from the University spree J. C. Rowell, to whom remittances should be addressed:— VOLUME 1. No. 1. The Geology of Carmelo Bay, by Andrew C. Lawson, with chemical analy- ses and codperation in the field, by Juan de la C. Posada : Price, 25¢ No. 2. The Soda-Rhyolite North of Berkeley, by Charles Palache : . Price, roc No. 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome Price, 4oc No. 4. The Post-Pliocene Diastrophism of the Coast of Southern California, by Andrew C. Lawson 5 9 Price, 40c No. 5. The Lherzolite-Serpentine and Associated Rocks of the Potreo, San Seas Francisco, by Charles Palache eanee No. 6. Ona Rock, from the Vicinity of Berkeley, ‘containing a New Soda Price; a6 Amphibole, by Charles Palache : 3 No. 7. The Geology of Angel Island, by F. Leslie Ransome, ‘with a Note on the Radiolarian Chert from Angel Island and from Buri-buri Ridge, San Mateo County, California, by George Jennings Hinde 0 . _ Price, 45c No. 8. The Geomorphogeny of the ‘Coast of Northern California, by Andrew C. Lawson : Price, 30c No. 9g. On Analcite Diabase from San Luis Obispo County, California, by Harold W. Fairbanks | : . Price, 25¢ No. 10. On Lawsonite, a New Rock- forming Mineral from the Tiburow Peninsula, Marin County, California, by F. Leslie Ransome . 4 Price, roc No. 11. Critical Periods in the History of the Earth, by Joseph Le Conte. Price, 20c No. 12. On Malignite, a Family of Basic, Plutonic, Orthoclase Rocks, Rich in Alka- lies and Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, by Andrew C. Lawson ‘ Price, 20c No. 13. Sigmogomphius Le Contei, a New Castoroid Rodent, from the Pliocene, Heater Berkeley, by John C. Merriam. . Price, roc No. 14..The Great Valley of paloma, a Criticism of the Theory of Isostasy, by \ F. Leslie Ransome . ‘ E Price, 45¢ VOLUME 2s No, 1. The Geology of Point Sal, By Harold W. Fairbanks ; pie 65c No. 2. On Some Pliocene Ostracoda from near Berkeley, by Frederick Chap- man . Price, 1cc No. 3. Note ou Two Tertiary Faunas from the Rocks of the Southern Coast of Vancouver Island, by J.C. Merriam . -~ -PHiceygroe No. 4. The Distribution of the Neocene Sea-urchins of Middle "California, and Its Bearing on the Classification of the Neocene Formations, by John C. Merriam 2 Price, Ioc No. 5. The Geology of Point Reyes Peninsula, by F. M. Anderson . Price, 25c No. 6. Some Aspects of Erosion in Relation to the. Theory of the Peneplain, by W. S. Tangier Smith 3 Price, 20c » No. 7. A Topographic Study of ‘the Islands of Southern California, by W. §. Tangier Smith . Price, 4oc No. 8. The Geology of the Central Portion of ‘the Isthmus of Panama, by Oscar H. Hershey : 5 Price, 30c No. 9. A Centenarian to the Geology of the John Day Basin, by John C. Merriam Price, 35¢ No. 10. Mineralogical Notes, by Arthur S. Hakle ; 5 Price, roc No. 11. Contributions to the Mineralogy of California, by Walter C. Blasdale Price, 15c No. 12. The Berkeley Hills. A Detail of Coast pape Gecloeys: ms eke C. Law- son and Charles Palache Z a a . Price, 80c UNIVERSITY OF CALIFORNIA PUBLICATIONS Bulletin of the Department of Geology Vol. 3, No. 22, pp. 423-475. ANDREW C. LAWSON, Editor THE RIVER TERRACES ORLEANS BASIN, CALIFORNIA Oscar H. HERSHEY. CONTENTS. PAGE HTirnitie LC G10 Migs rece See etc sas cx stacey ete traces ox eeteas se eaeeyecesacee teeteea sass Pe ore: yp (Ap Vaysy LRA ayeL EAST Comey rd aed eet sy ea Ke) 08 Nee ey seer pee Rae eae tee er ere eS yee are 424 iBriet Outline: of Geomorphogony =. ..2cc2ccsceqceceeesececeseecceseseeceeececceseearaeedes sereeaeo= 424 Detailed Description of Terrace Remnants.............20. 22 ceeeteee cette oe 428 MherS50—foot LeErrace: 2. .......c-sceceecvee se -e--casreceeres OE A OE RS, Ee 428 The 675-foot Terrace The 475-foot Terrace Tue wli? O=LOO tm CTUA CCl ats. cate sesrtets coer =: cceb ese. tett es sas ontndacasu dete 22S tee nscareer eee eaes 433 MMe mO=£0 Ob) MOLY ACO .2.5..2.c2.cc< However, on the Isthmus of Panama, I found a deep or blue.’ red soil prevailing in the dense jungles, even where the under- lying rock was blaek, gray or yellow, while on the grassy plains that are dry half the year, unless the underlying rock was red, the soil was never of that color. Red and other bright hues occur on deserts, but it is not the brick red tint of the moist tropies. The prevailing colors of desert soils are ashen gray and hght brown, unless the underlying rocks are red. It is a question whether the red color of the upper terraces was original or has subsequently been produced by oxidation. One fact leads me to think that the flood-plain silts were depos- ited red. The color is uniformly reddish brown (except in the few places where it is dark blue beeause of deoxidation on account of the presence of much drift-wood), and these silts preserve this color where they pass under thick masses of gray slate debris or green serpentine landslides. If originally red, it implies that the river drained a country having a prevailingly red soil. Whether the red color of the silts was original or subsequently produced, it indicates a comparatively warm and not arid climate for the earlier portion of the terrace period. In fact, these red silts occur down to the seventy-foot terrace. *Bulletin No. 52, U. 8. Geol. Survey. + Monograph No. 14, U. 8. Geol. Survey, pp. 7, 8. 464 University of California. [Vol. 3. The dark brown color of the flood-plain deposits of the forty- five foot terrace is due to the presence of much carbon. The soil was prevailingly dark brown. It imphes a luxuriant vege- tation and a cool, moist climate. As I will correlate this lower terrace with some portion of the last great glacial epoch, it will appear that the lowering of the temperature which caused the ereat extension of the Wisconsin glaciers, changed the soil of Northwestern California from red to brown. Since the glacial period has terminated the soil has gradually become lighter in color, as evidenced by the lighter tint of the Modern silts. Professor D. P. Penhallow’s report to Mr. Knowlton on the fragments of wood from the Ferris and Wilder Mines is as fol- lows. Set No. 1 is from the Wilder Mine, and Set. No. 2 from the Ferris Mine: ‘‘T have completed an examination of your specimens and have to report that they are all Coniferous. They present some interesting features of preservation, which I shall discuss at a later date in another connection. I have numbered the speci- mens from 1-7. No. 3, Set No. 1, is Pseudotsuga macrocarpa. No. 4, Set No. 2, is Juniperus californica. Nos. 1 and 2 of Set No. 1 represent a species of Juniperus which could not be determined on account of structural altera- tions, but there is reason to believe it may be J. californica. No. 5 of Set No. 2 is not determinable, owing to the very high state of alteration, which would not permit of sectioning. Nos. 6 and 7 of Set No. 2 are either Pseudotsuga, Picea or Larix. It is impossible to decide definitely between them, but the probability seems to lie in favor of the first. With respect to the relation to existing representatives of the same genera, it is to be noted that Pseudotsuga macrocarpa is still extant in the same region. Juniperus californica appears to have receded somewhat toward the south, as its northern extension is at present confined to the valley of the Sacramento, thence southward along the Coast Range. While these facts are not in any way conclusive, they suggest the possibility that present conditions are slightly more boreal than during the time our trees were living. This would seem to agree with the Hersuey.] The River Terraces of the Orleans Basin. 465 evidence of fossil representatives of Pseudotsuga and Sequoia from other regions of the West, which shows a definite recession from previously occupied areas.”’ The most startling result of this study is the discovery of practically conclusive evidence of a comparatively short period of excessive rain-fall. This was first suggested by the torrent fans on the 120-foot terrace. It must be remembered that these fans oceur only at the mouths of such small ravines as did not produce similar fans on any higher or lower terrace. Corre- sponding fans in the mountain gulches away from the river are so coarse and so peculiarly ridged along the central line leading up the small gulches as to imply rapid formation as the result of eloud-bursts. Now, cloud-bursts are characteristic of arid climates, and for a time it was a question in my mind whether these torrent fans indicate excessively humid conditions or semi- arid conditions. I could not find any satisfactory solution for the problem until it occurred to me that the landslides furnish the key. ; It is a remarkable fact, established by abundant observation, that the great majority of the landslides bear an intimate rela- tion to the 120-foot terrace. A few landslides oceurred earlier, and some later, even down to the historical period, but the larger landslides, and by far the greater number, occurred during a short period which was identical with the torrent fan period. In this connection there are three hypotheses worthy of consid- eration: 1. That in cutting from the 475-foot to the 120-foot terrace such high, steep slopes were produced as especially favored land- sliding. The objections to this are that many large slides along the serpentine belts moved several miles, and from positions not at all affected by erosion below the 475-foot level, and that these landshdes did not occur in considerable numbers until after the upper channels under the 120-foot terrace were completed. They clearly date from a particular portion of the time occupied in forming the 120-foot terrace. 2. Many of the settlers attribute these landslides to earth- quakes. The region is one of the most stable on the continent, and, so far as [ am aware, no severe earthquakes have been expe- 466 University of California. [Vol. 3. rienced here within the historical period. There is no collateral evidence of a period of severe earthquakes in the latter portion of the Quaternary Era, and, besides, I doubt the efficiency of a series of earthquakes to produce the phenomena observed. 3. The hypothesis which I accept is that the landslides con- neeted with the 120-foot terrace are due to the same abnormal climatie condition as produced the torrent fans. This condition was one of excessive rainfall. Cloud-bursts with prevailing sem1- arid conditions would not soak the earth to a sufficient depth to eause such a general landsliding. It required long, heavy rains. This season has been one of abnormal precipitation. From the 3rd of February to the 29th of March there was almost contin- uous storm, and about forty inches of rain fell in Orleans. Many of the smaller landslides settled several feet, but no large ones were formed, and no torrent fans similar to those of the 120-foot terrace. The torrent-fan and landslide-forming period must have been one of almost continuous heavy rain for months, with frequent cloud-bursts. It was almost of a cataclysmal nature— a sort of incipient ‘‘Deluge.’’ I am a firm believer in the usually mild processes of Nature, but we certainly have evidence here of something abnormal. During this period of excessive precipitation, the river occu- pied the lower channel under the 120-foot terrace. The gravels of this channel are markedly coarser and thicker than those of preceding channel. This is due largely to the coarse debris thrown into the channel by the landslides and coarser torrent fans. The river must have been greatly increased in volume, other- wise the sudden influx of this coarse material would have caused its channel to be aggraded much more than it was. Thus the conditions of the channel furnish corroborative evidence of excessive rainfall. ; This supposed period of excessive humidity appears to have immediately succeeded the maximum extension of the glaciers of the so-called Intermedite Stage. It is probable that the warm rains caused the glaciers to be rapidly melted away. If I am correct in correlating these ‘‘Intermediate’’ glacial deposits with the Iowan drift of the Eastern States, it will appear that the period of excessive rainfall in the Orleans Basin was identical oe ? Hersury.] The River Terraces of the Orleans Basin? 467 with the period of deposition of the Iowan loess in the Missis- sippi Basin. This suggests the idea that the loess may have been due to more abnormal conditions than simply a subsidence of the region. Relative Age of Different Terraces.—In comparing the canons excavated between the different terrace levels. [ will ignore the alluvial deposits. he time occupied by their removal is a very small fraction of the entire period of canon cutting, and consequently they introduce a needless compheation into what will at best be a very rough computation. By inquiring among the Indian fishermen and others who are acquainted with the river, I have derived the estimate that the average depth of the bed-rock below present low-water mark is about ten feet, and as the bed-rock floor of the forty-five- foot terrace averages ten feet above the river, twenty feet may be assumed as the average depth of the Modern rock-canon. The most delicate part of this discussion is the determination of the probable age of the Modern canon. We have no natural chronometers, such as are constituted by Niagara and St. Anthony Falls. Extensive inquiry among the old settlers has not yielded very definite results. However, it is certain that the cahon has not been eroded within a period of several hundred years. By reason of the placer miners’ tailings, the river has been agerading its channel for some years, but that does not prevent it from eroding the banks. In 1860, and again in 1890, severe winters caused many landslides along the river, but, con- sidered as a whole, there has been no appreciable widening of the channel in the past fifty years. ; Less than one-half mile downstream from the Orleans post- office, and on the same side of the river there is an old Indian village site. The edge of the bank is about twenty-five feet above the river, and a gentle slope leads back from it to a flat plain which is about 250 feet wide and has a height of about thirty-five feet above the river. Back of it, another gentle slope leads up to the flat plain of the forty-five-foot terrace. The lower terrace is composed mainly of a deep bed of dark brown sand. Similar sand beds occur at this level at various places alone the river, and they are usually essentially non-pebbly. But at this 468 : University of California. [Vol. 3. place the sand contains great quantities of river cobbles, very many of which are broken. They are seattered about on the plain over a space fully 200 yards long by 100 yards wide, and patches of them occur on the higher terrace. Along the bank where the river at flood times is eroding the sand into a perpendicular bank from three to six feet high, it is seen that in places the cobbles only extend to a depth of two feet, but in others are thickly packed to a depth of five feet. By the removal of the sand the cobbles accumulate at the foot of the bank, where they form extensive beds. They attract attention by reason of the comparative uniformity in size (by far the larger number being three or four inches in the longer diameter), and by the large proportion that are broken. Many of them are reddened by fire, and nearly all are supposed to have been used in cooking acorns, by whieh they became brittle and were easily broken. Along with these cobbles there are many angular fragments of white quartz, and occasionally an obsidian flake, but implements are not common, although I am told that mortars and _ pestles have been found. The remarkable feature of the deposit is the ereat quantity of these old cooking stones. It is no exaggeration to assert that hundreds of thousands are now exposed to view at the foot of the steep bank, and many times as many may remain buried in the sand of the terrace. From imquiry among the Indians I learn that each family used from five to ten stones ina set. It is a question of how frequently they were broken and how many families lived in this village, but it is beyond doubt that this site was occupied for many centuries or else the population was very great. Yet this village dated entirely from a time subsequent to the abandonment of the forty-five- foot terrace by the river, and was nearly unoccupied half a century ago. : IT am strongly inelined to consider the uplift to which the Modern canon is due as also the cause of the great extension of the glaciers in the last, or Wisconsin stage, and on this suppo- sition the age of the Modern canon may be placed at 5,000 years. However, this figure will imply an unreasonably great age for the upper terraces, and, in place of it, I will arbitrarily assume 2,000 years as the age of the Modern canon. It is not my inten- Hersuey.] The River Terraces of the Orleans Basin. 469 tion of pretending to approximate closely to the age of the ter- races, but simply to fix minima which everyone can accept. Basing the estimates solely on the depth of the erosion, we will get the following result: The rock canons have depths respectively of 20, 35, 45, 315, 200 and 120 feet. The corre- sponding periods of time will be 2,000, 8,500, 4,500, 31,500, 20,000 and 12,000 years, or a total for the terrace-forming period of 73,500 years. But the above is obviously not a fair estimate, as it fails to take into account the very important factor of different widths of the several canons. I will allow the Modern canon an average width of 750 feet, which is a liberal estimate. With higher eanons I will be more strict in my estimates. The upper two may be considered approximately equal in width, because the lower occupied as much new territory as it left in the form of the 675-foot terrace. The average widths of the canons are respectively 750, 1,500, 2,000, 3,000, 5,000 and 5,000 feet, and the corresponding cross- sections, 15,000, 52,500, 90,000, 945,000, 1,000,000 and 600,- 000 square feet. By this method we derive as the length of time oeeupied in the formation of the canons, 2,000, 7,000, 12,000, 126,000, 133,0004+- and 80,000 years, or a total for the terrace-forming period of 360,000 years. The age of the 120- foot terrace, which I correlate with the Intermediate glacial deposits, will thus be 21,000 years. This agrees fairly well with estimates of the probable age of the Iowan drift of the Missis- sippi Basin, and constitutes another point in favor of consid- ering the Intermediate drift as pre-Wisconsin in age. The last estimate of the age of the respective terraces seems large, but is probably fairly conservative. It is based on the supposition that the abnormally rapid rate of erosion of the high-grade Modern canon obtained throughout the terrace period. However, it is a well-known fact that the rate of erosion ereatly decreases as the valley widens and the gerade lowers. Taking this into consideration, it is probable that the age of the Modern canon could be cut to 1,000, or even 500 years, without necessarily reducing the age of the 850-foot terrace below the 360,000 years which I have assigned to it. However, 470 University of California. [Vol. 3. I will arbitrarily reduce the assigned age of the highest terrace to 250,000 years. The portion of the Sierran Canon above the 850-foot terrace is more than three times as deep as that below, several times as wide, and has characteristics indicating a much ereater age. It is undoubtedly conservative to assign it a period of erosion not more than three times as great as the age of the highest terrace, or 750,000 years. This yields a total age for the Sierran Canon of 1,000,000 years, and that figure also represents my idea of the probable length of the Quaternary Era. The Sherwood Valley has the appearance of being at least five times as old as the Sierran Canon, or 5,000,000 years. The geologists who are working in the Pacific Coast country are inclined to assign much longer periods of duration to the Plio- cene and Pleistocene than do those whose field lies in the Eastern States. Recently Dr. A. C. Lawson has given* as a_ possible duration for Quaternary time, 2,751,000 years. However, he includes in the Quaternary the period of erosion of a series of ‘‘Hich Valleys’? of the Upper Kern Basin, which valleys appear to me to be the correlatives of the Sherwood Valleys of the Klamath region. My figure corresponding to his given above is 6,000,000 years. For several years I have entertained the idea that the Sierran Canons have been in process of erosion for at least a million years. I have been diligently searching for evidence of rapid erosion, and in general have secured only negative results. I will not deny that in places the streams are actively under- mining steep slopes and causing landslides, but the total amount of material thus removed in a century is very small. Along the South Fork of Salmon River there has been little change in the positions of large boulders in half a century. Fir trees 300 years old frequently stand on low Modern flood-plains in the small gulches. On the steep mountain sides, although the sur- face debris is very loose and apparently in movement down the slopes, there can be little lowering of the surface in a period of 100 years, as may be determined by an observation of the timber. The debris accumulates against the upper sides of *Bull. Dept. Geol., Univ. Calif., Vol. 8, No. 15, p. 368. Hersuey.| The River Terraces of the Orleans Basin. 47] large trees and slides away from the lower sides, thus furnishing a means of a fairly good estimate of the rate of movement of the surface debris. Trails which were established fifty years ago, and not repaired sinee, have a curious and agera- vating serpentine course. Where they passed above trees they remain in their original position, but between the trees they have worked down the slopes from several to ten feet. By a eareful study of these trails it is learned that there has been a continued movement of the debris down the slope, but it has been very slow. Trails which are not used during the winter months are not severely injured unless locally by landslips. Abandoned trails on steep slopes are not obliterated for scores of years. Large trees occur on narrow mountain summits, and demonstrate that in general these summits are not lowered one foot in a century. If the Klamath Canon was now being enlarged at a rate sufficient to have produced it in 100,000 years, the timber could not maintain a foot-hold on its slopes and it would be uninhabitable. The Pleistocene erosion through- out the central portion of the Klamath region is equivalent to the removal of a sheet of very resistant rock from 500 to 2,000 feet thick, and all of this material was passed out through the mouth of a single stream that, before the arrival of the placer ‘ miners, was ‘‘clear as crystal’’ nearly all the year. One million years is a conservative estimate of the time required. CORRELATION. For the purpose of correlation, only three of the terraces are important, namely, the highest, the 120-foot and the lowest. Remnants of this system occur in all the principal valleys of the Klamath region, but reach their finest development on the western slope, near the coast. The small Modern canons are characteristic of the country west of a line whose course seems to be a little east of north, and whose position is just west of Seott Valley, nearly midway between Trinity Center and Summerville, and traverses the Trinity River, probably near Junction City. This is the axis of the uplift to which these canons are due. Now, two large rivers, the Klamath and Trinity, rise east of the axis and cross it. The 472 University of California. [Vol. 3. Scott River, below Scott Valley, crosses the axis. Lawson has called my attention to the fact that the broad-floored Scott Val- ley presents strong evidences of being an aggraded valley. It appears that the arching across the lower Scott River has been so pronounced that the stream has been unable to cut: a cation through it down to an average grade, and a filling of Seott Valley has resulted. The Upper Trinity Valley, lying east of the axis, also shows evidence of aggrading, but to a less extent than Seott Valley. For fifteen miles the Upper Trinity River, instead of flowing in a small canon, has a Modern flood-plain that averages a quarter of a mile wide. The maximum elevation seems to have been at a point near the head of the South Fork of Salmon River, where the moun- tains are now highest and the glacial phenomena of the last stage most intense. West of the axis the tilting seems to have been toward the west-southwest. The lower terrace seems to be higher where the streams are flowing in that direction than where they are flowing northwest. This is only a suggestion, as very little accurate information on the subject is available. Last year I discussed* the terrace system as it is developed near Summerville, in the valley of the South Fork of Salmon River. The highest terrace (that over Channel A) of the Sum- merville Basin corresponds to the 850-foot terrace of the Orleans Basin. Associated with the former there are apparent very old elacial deposits, representing the first glacial stage. The 120- foot terrace of the Orleans Basin has its counterpart in the terrace over Channel C of the Summerville Basin. The latter has a similar height and the characteristic coarse torrent fans. I traced it into direct connection with deposits of the Interme- diate glacial stage. I want to emphasize the fact that in two distinct areas, thirty-five miles apart, I have found glacial deposits closely related to a terrace which has unique characters. Being mutually corroborative, they greatly strengthen the hypotheses of a short period of excessive rainfall immediately following the maximum extension of the glaciers in the Inter- mediate stage. The lowest terrace of the Orleans Basin is the correlative *Journal of Geology, Vol. XI, No. 5, July-August, 1903, pp. 431-458. Hersuey.] The River Terraces of the Orleans Basin. 473 probably of the terrace over Channel E of the Summerville Basin. I eannot correlate these lower terraces with the glacial series except in a general way. It is my impression that the seventy-foot terrace represents an early sub-stage of the Wis- consin glacial stage, and the forty-five-foot terrace a late sub- stage of the same epoch. Throughout the Klamath region the highest terrace is char- acterized by fineness of materials and the red color. It seems to attain to its greatest height along the Klamath River between the mouth and a point above Happy Camp. Im the valley of the Trinity River it rarely reaches 300 feet above the stream. In Seott Valley it is very low and indefinite. On Clear Creek and the Sacramento River above Redding it is fairly well repre- sented, but at heights usually less than 200 feet above these streams. I wish to eall particular attention to one fact in connection with this upper terrace, namely, that it marks an important line of division of the Sierran Canons into a comparatively broad, upper non-terraced portion and a narrow, lower terraced por- tion. The contrast between the two portions is great enough to point to a change in conditions. The latter portion of the period during which the upper division was being eroded was a time of quiescent conditions. There were no important changes of level or of climate, and the streams had lone cut to low grade and greatly widened their valleys. The upper terrace is simply a portion of the valley floor at the close of that quiet period. The remainder of the Quaternary Era has been one of repeated earth movements and changes of climate, and the terrace system is the result. In much softer formations than those of the Klamath region, the broad upper canon would be represented by very broad. basin-like valleys, or even, on incoherent late Pliocene strata, by small peneplains. In the softer rocks of the Coast Range province, the Klamath River could probably have exeavated a valley 2,000 feet deep and fifteen miles wide in the time which has oceupied it in eroding the upper division of the Sierran Canon. This fact must be taken into account in correlating valleys and terraces throughout the State. 474 University of California. | Vol. 3. The 850-foot terrace of the Orleans Basin I will correlate with the Red Bluff formation of the Great Valley. This is based on the fact that the highest late Quaternary terrace of the Klamath region may be traced out of the mountains, and it becomes the prominent Red Bluff terrace on the northern border of the Sacramento Valley. The internal structure and the history involved in the Red Bluff formation have not yet been thoroughly elucidated. The Red Bluff proper is eompara- tively old, as is evidenced by the undulating topography of most of its area. North of the latitude of Sacramento it has the deep red color which is characteristic of the upper Quaternary ter- races of the neighboring mountains. So far as I am aware, there are no Quaternary terraces higher than the Red Bluff on the borders of the Great Valley. It marked the end of a long quiet period and the beginnine of the disturbed, terrace-forming period. Taking all these facts into consideration, I believe that the correlation of the Red Bluff formation with the Quaternary terrace of the Klamath region is fairly safe. In 1902 I discussed* a system of river terraces carved on a late Pliocene series in the valley of the Santa Clara River of the South, in Los Angeles County. The highest, estimated at 400 feet above the river, marked the end of a long quiet period (during which the Pliocene Basin was almost reduced to a peneplain), and the begining of a terrace-forming period. On the principle that the Quaternary history of the Klamath region was in a general way duplicated throughout the State, I must correlate this 400-foot terrace of the Santa Clara Valley in Southern California with the 850-foot terrace of the Orleans Basin. Before I had gained the idea that the highest late Quaternary river terraces in all portions of the State should be considered equivalent in age, I had referred the 400-foot terrace mentioned above, and the highest terrace of the Sierran Canons of the Klamath region to the Red Bluff epoch on the basis of erosion studies. In short, the upper division of the Sierran Cafion at Orleans must be referred to the Santa Clara epoch of the classification “<¢The Quaternary of Southern California.’’ Bull. Dept. Geol., Univ. Calif., Vol. 3, No. 1, pp. 10-11. “| o HERSHEY. | The River Terraces of the Orleans Basin. 4 proposed in the paper just cited, the Red Bluff horizon occurs at the 850-foot terrace, the space between this terrace and one at least as low as the 120-foot terrace represents the Los Angelan epoeh, the San Pedran horizon is due at or near the seventy- foot or 120-foot terraces, and the Glacial epoch is represented probably by the forty-five-foot terrace and the space between it and the seventy-foot terrace, and probably also by the latter. During the first few years of my residence in California the river terraces did not appear to present any interesting prob- lems, but the deeper I delve into their history, the more fasei- nating grows the study. They are important because they indi- eate orogenie disturbances and changes of climate, and because by means of them we will be furnished the best chronometer of elacial events. It is possible that they may yield facts bearing strongly on the cause of the great Quaternary glaciations. They furnish the basis for the classification of Quaternary land faunas. Further, the relies of early man in California may be referred to the different terraces, and thus some idea gained of their relative ages. So far, in the Orleans Basin, I have failed to secure authentic evidence of the presence of man until after the completion of the forty-five-foot terrace. Mr. Pearch reports that he mined out an Indian mortar from a depth of twenty-five feet below the seventy-foot terrace level, but there is no certainty that this mortar did not come from near the top of the bank. Berkeley, California, May 25, 1904. INDEX TOP VOLUMES: Novr.—Italicized page numbers indicate maps or illustrations. Page AGASSIZ, L., cited On Nemacanth us. 399 AGGRADATION of channel of Klamath , Kern Cafion, by glacial action , Scott Valley.. SS —' Upper Trinity Valley ALBITIT ES ALGONKIAN, use of term criticized ANALYSES: PAMIOTONILSS ccc ccerdvsranueresatecesenu sane 394 —, Aplite..... 190 —, Augite, diorite.. 8 —, Boothite —, Chalcanthite. —, Copiapite —, Corundiferous rock —, Diorite.... —, Epsomite —, Feldspar......... —, Gabbro-diorite ..... , Hornblende-gabbro. —, Hypersthene andesite , Mascall tuff —, Melanterite —, Orbules from gabbro —, Palacheite —, Pegmatite........ = , Peridotite —, Quartz-basalt , Recent ash, John Day Basin —, Rhyolite —, Spodumene. ANDESITE..... 172 ANIMIKIE SERI 54 ANORTHOSITE SI ANTELOPE VALLE y, ‘described . 20 ANTISELL, T., cited on base of Miocene... 379 REED Eoaeet tnateeasssaaledigecesnde ssesai eer 181, 297, 388 ARCH4ZAN GNEISS oe ere —, term defined.. 53 ARNOLD, R. marine Pleistocene studied by 2 = ARZRUNI, Awe cited on colemanite............ eh ASHLEY, G. H., cited on sediments under Miocene 79 ATRACTITES BEDS . 67 PASTTG ITs CATS VCE yecepeesp ceeesessceeesterecceese 221 BACON FLAT river terrace BASALT.. BATHOLIT . BAurR, G., cited on rehehcosauria BEACH CREEK serpentine ....... 120 BERGSCHRUND -. 358 BIG ARROYO CREEK 306 BIOTITE-syenite, corundiferous 221 BLUE MOUNTAIN RANGE ABAEBRES BODEWIG, C., cited on colemanite.. 32 BONNEY, cited on fibrous pseudomorphs in volcanic rocks BRAGDON SLATES.... 424 BREZINA, cited on pisanite 206 BROWN F var gravel deposi 432 BRUSH, cited on spodumene.. 273 BURNT CORRAL MEADOW, terrace near 326 BUTLER CREEK VALLEY, glacial deposit of 452 Page CAJON Pass, Quaternary alluvial fan at... 24 CaxLico District colemanite locality es CAMB RUAN ES Ey Rui sleds: rccetstadsesestarceceee 2 CANIDAE, Pliocene and of Great Valley CANON CiTy LEAF —, of Klamath River — —, Upper Kern River CARLSBAD TWIN CHAGOOPA PLATEAU CHELOYIAN eggs of ‘I CHERRY CREEK andesitic tof. —, basalts CHICO FORMATION...... CHINECH CREEK, landslide deposit. CIRQUE PEAK CIRQUES f 3: CLARNO FORMATION....... CLARNO’S FERRY andesite CLIMATIC changes in Orleans Basin. Quaternary COLEMANITE...... 31 —, Combinations . 38 —, Crystal Habit 50 —, Elements.......... cn eK == POLIS, CADIS .cceaav stevens scenns 3 : 6, 48 —, Method of measurement ...............2.0005 40 —, Occurrence 32 —, Polar Orientation... 4i (Pay Ee YOUCCHONS cc. pues. ccsstsaxence 50 —, Record of measurement 45 Contact between granite and mentary rocks.............. + 209 Cope, cited on Borophagus CORUNDIFEROUS ROCKS... 219 —, dyke cutting peridotite 222 ——(—WEXUGIIUl erssiecenepecsees? 225 —, facies of dyke rock ... 225 —, rocks, chemical composition of 227 — —, type defined 227 CORUNDUM PEGMATITE.... 220 , syenite +5220 COTTRELL, F. G., cited on manganese SUP MATES isessascsasees 211 COUTCHICHING SERIES 60 CRETACEOUS CLAYS 313 —- dni John! Day BaSiny o-os.cecorsr-siecesecusnees 112 CUAHILLA, near spondumene locality ...... 265 CURRANT CREEK HILL spherulitic rhyo- VICES cc ccen cesaesceastanewiavereasnaces nnavancane pee 7 DANA, cited on spodumene .. yk DARAPSKY, cited on rubrite . 236 DEATH VALLEY, colemanite locality 32 DEHESA, orbicular gabbro at............ +» 383 DELTA extension in Upper Kern Lake...., 345 DESOLATION CREEK Serpentine............... 121 DETRITAL slopes of Red Bluff age ........... 23 DIFFERENTIAL degradation in Caucasus... 313 ——, in Kern River Region... ais DIFFERENTIATION of igneous magma 190 DILLER, J. S.. cited on magmatic resorp- tion . 135 DIORITE 266 —-—,ga 188 DISINTEGRATION of granite . 207 DONAHUE CHANNEL near Orleans............ 429 (477] 478 cited on coquimbite ........... 232 discoverer of plumasite EAKLE, A. S., EDMAN, J. A., LOGCALLEY \acccivsscessedesscvarscacenstnn renee 221 EPARCHAEAN INTERVAL, defined . SA) EROSION interval below Penokee Series... 59 — studies, discussion of methods .. 13 ERRONEOUS CORRELATIONS in “Lake Superior Province 57) ESCONDIDO SERIES éicsrecsierseense 2 EXCESSIVE PRECIPITATION, period of in Orleans Basin FAIRBANKS, H. W., cited on geomorpho- geny of Sierra Nevada... 6 ———, marine terraces ... 27 ———, Point Sal Miocene ...... 379 — ——, rocks near Dehesa, Cala 384 ———, spodumene- bearing dyke. 266 ‘Triassic beds of Shasta County..... 65 FARRINGTON, O. C., cited on fossil “egg FLOM Mi0CeN ...ceeeeeeesesseseseeseseeseeese ene FAULT in Kern Cafion.. FAULTS oe FERRIS CHANNEL.. —, Mine, fossil wood m4 30 Fossiuiege from ATiZONA .....-cscss.50ssa0s 403, g10 FOSSILS : = A EKOCIOKALCEV ES: iapccexevssansessay svdsatans tonnes 67 —, Aelurodon ...... 282 — —, SAeUVUS ........ 286 — —, wheelerianus ... 286 —, Agasoma gravida 378 — =, SENUALA.....000004 380 —, Ammonites blaket 104, es AVEO ay sev is vauay can eiiexesseeiteg mie eye! —, Arcestes CAILPOYNICUS «0... 0ecee ees zs 66 —, Arpadites cinensts ... . 65 —, Asteracanthus .... 543/399 —, Atractites ...... if 67 —, Aulacoceras . 67 —, Balatontites . 65 —, Babtanodon. 252 —, Benecketa? 66 —, Borophagus 280 — —, diversidens. . —, Canis indtanensts — —, latvans ......0 ——, lupus..... fee erm PT LIN LEU Sie stan sea eos see anne cris iesereaes cs 288 —, Capulus .... 66 NGELLZLES = ; = =) Cephatogale. 3 , Chione mathewsont 378 , Chrysodomus 378 y GEAALIS..ssnn10000- 68 , Clemmys gutta la. 239 Er ESPEXIG eae - 240 —-- —, LEDYOSA se .csesee vo0 + 240 — —, marmorala... 238 — —, Sarena , 241 —, Clypeaster brewerianus 378 —, Cosmacanthus .......-. 400 as COPY DONAILUS: sce vsuieavsdecsdcnaeeusdeeseeasses saeen 400 a — CCLEC OSs ca asestaccacneecnaseneucereumeenese? 398, 402 — —, malcolmsont.. ss. 4O0O —_--, seh Sp LES 400 — —., Stellatus . 400 —, Crepidula.. F recy = Crmbospondyh 104, 251 = "— grandis... ...106, 109 — —, petrinus ..106, 09 wens oars, PESCOSILS. coawapensuetecensnsiasncaceddueeasnss 104, 109 ——=. JJOSLEN1G MLALEWUSONT acecceasevaciscescssverasssaes 378 University of California. FOSSILS : Page —, ELUCEKALHEKTUML vacecvres aorcsorsesceecoseoncences 411 — —. collinum.... —,. PeILOMOCEKAS SAN GLIENLEUSE saeuvaceas: Wire 67 5 PLCUIG ca oaascateusesneerse=rec 378 —, Getsacanthus ++» 400 —, GEV ULNA cas ccsese 68 —, GLYCIMEPTS «2.60000 378 —, Glymmatacanthus .. 400 —, Halorites ramsauert . 67 —, Halobia superba .. 66 —, Haplocerus.... 414 —, Homaeosaurus —, Hyaenognathus pachoy —, Hyanognathus? AUb Us.cccccccceccceceeees 283, 290 —, Ichthyosaurus — —, carinatus.. — —, hector?.. — —, polaris.. ——, rhaeticus ..... —, Juniperus californica LOY aes ee —, Lecanites . —, Leda taphria. —, Leptochetru —, Margarita. —, Meekoceras.... —, Mixosaurus . — —, Atavus... — —, cornalianus — —, nordenskjolat. —, Modiola........... —, Mylodonr ....... —, Mytilus mathewsont . —, Nannites spurtus . —, Natica «2... —, Nautilus trtadicus .. —, Nemacanthus monilifer ma LNCUEKILG) a assencsieccasonees —, LOLMSQUPUS ..02.0200: 250, 253, Nucula divaricata Olivella pedroana . OPHICETAS cisiciescessn Opthalmosaurus Oracanthus Orthoceras Ovtbos ..... —, Palaeocyon ..... —, Fecten peckhamt —, Pentacrinus..... wt PLCED cic tianvesens —, Polycyclus henseli . —, POKthOCYON ....1ecevevseees —, Posidonomya stella .... — —, WENGENSTS ...... —, Prinolobus .... —, Proterosuchus.. —! Pseudosageceras... es —, Pseudotsuga macr ocarp z = LLY C/ULLOS aecvesceeeseer seein —, Rynchonella solitaria =) SOL CCEF ES) ceceseschestses —, Sagenttes evinaceus —, Shastasaurus oi... ——, alexandrae.. ——, alltspinus.. =, COVERT ath an neatsatpacesteses =, OSHONEL Jcossaseiveeeneens — —, pactficus.. ——, perrint.... —, Sphenodon .. —, Spriferina .... —, Stylemys calauvi Ss. =) LEA A COUG ESA ssassansensssstsasceveseveseememee —, Terebratula ..... A —, Thalattosaurus suse 420 — —, AlEXANAPVAE.....06cceceecees gcssanavecesasee .419, $20 Index to FOSSILS: —, Trrolites fotlaceus . —, Toretocnemus .... — —, californicus —, Trachycere ——, aon ——-, aonte — —, archelaus ——, armatum ——, hylactor . — =, ladtnum ...ccc. ; —, Trochita costellata. 378 —, Tropides Janus.. 66 — —, salurnus 67 ——, subbullatus... 67 —, Turritella... 378 —, hoffmant 379 — —, ocoyana 379 VOUS cnn cenuncccsabyees 378 Fossi_ TURTLES from Oregon, 237 FRASER MOUNTAIN. Meek 34 FUNDAMENTAL GNEISS . manesins 52 Gasp, W. H., cited on upper member of INIGOGEN Gincarenss testa: cteccerscasen. sabe nearecee GABBRO of Upper Kern Basin . —, orbicular.. —, uralitic .. GILA RIVER GRAVELS, fossil egg fr om GILBERT, G. K., study of Upper Kern Basin Fu suuessers Muisaamcas ceils Nesesice doen ssthe - 292 GLACIAL BASIN on Orleans Mountain - 452 —, Deposit, presumed lowest in California 454 SEG DOC, a secietscdarsasnvane ceuabaeedecnsuaunres 27, 28, 475 — Grooves 350 — Reduction of mountain cres 359 — Sculpture in high mountains 358 GLACIATION in Upper, Kern Basit 366 GLACIERS, living in Sierra Nevadas......... 366 (GRIABEN anit covatsceca seas ccsveuces tr esesees Serre 336, 339 342 GRADE OF KLAMATH RIVER changed in Quarternary time .... ——, Upper Kern River GRAHAM FLAT gravel deposit GRANITE-PORPHYRY GRANITIC rocks of Upper Kern Region GRANODIORITE . Grant, W. T., cited in Upper Kern Lake 344 GREAT WESTERN DIVIDE .. — ——,examplification of glacial erosion 361 GREGORY, cited on fibrous pseudomorphs in voleanic rocks. 125 GRENVILLE SERIES.. 52 GU VODRMDan eres cceeestietcttstectsecivss: 05 HALD’s CANON andesite ........... .ccccseseeeeens 128 HANGING VALLEYS of Kern Region G29) G52 Bt —— OTLCA MS BASU og aiscccsenessee ss cevcss oscuine 454 HERSHEY, O. H., cited on subdivisions of Quarternary .. 368 HERZ, W., on salvadorite. HIGH MOUNTAIN ZONE of Upper Kern IBASIwscecerascert st cate et eae e eavbaderasie 306 — Valleys of Upper Kern Basin... 315, 327, 470 HINTZE, cited on PISATIIUCN oscsscce os eeeess cts eie 206 HIORTDAHL, 'T., cited on colemanite....... 32 HOLLAND, on corundum syenite in India.. 220 HORNBLENDE-BIOTITE granodiorite ...... pan 3 70 HORNBLENDE-GABBRO. 385 HOSSELKUS LIMESTONE, described . as, (05, =, TelAtions Of falta! ..cccssevasecsessccoscesscceecs 68 ICHTHYOPTERYGIA, bibliography ............ 108 Triassic, from California and Nevada.. 63 ICHTHYOSAURIA, Upper Triassic of Cali- POTN A ee ceneefeseeecrerarsncneieereee steaks jesus: 2AQ) Volume 2. 479 Page IDDINGS, cited on magmatic resorption... 135 IGNEOUS ROCKS near Pajaro........ SpE 173 — — —, Acid dykes 181 — — —, Basic phase 179 —— —, Characters of main mass 177 — — —, Chemical characteristics, tables.. es .184, 185, 186 — — —, Geological relations 174 — — —, Graphic representation 188 ;Nonienclature..-.-...- — — —, Petrographical typ INDIAN MorvrarR found near Orleans. — Village site near Orleans INTERMEDIATE glacial stage .. ISCHAPISCHA FALLS ..._._.. Piceenes ISTHMUS OF PANAMA, red soil of ............. d Jackson, A. W,, cited on colemanite aS JOHN DAY BASIN, Clarno Eocene of 2 a MEO OC IEIONIS LO) ay gucccsaassccatvesusuwescey) —, Lavas of.......... ; , Mascall Formation . —, Miocene basalt . —, Miocene of —, Petrography —, Pre-Tertiary geology —, Quaternary s — — —, Rattlesnake Formation... 114 JOHNSON, W. D., cited on glacial destruc- tion of mountain crests 357, 359 JOINTAGE, curved 303 —, Kern Region. 352 —, Mt. Whitney 302 —, Yosemite Valley 302 JUNCTION PEAK ae iar G00 JURASSIC LIMESTONE of Caucasus..... ...... 313 KAWEAH PEAKS, metamorphic rocks of... 298 EEE NB UBS bee Semen set eenes eect Tey 331) 365 —, compared with rock-slides .......... : 335 ==, Rift hiv poth Sisiofe eo. sesseeserseneees ee 336 KERN CANON, glacial action .. — —, profile KERNCOLS ... Manse ED KEWEENAWAN SERIES : KING, cited on John Day Beds . Ay 180) modification by ty OO 0 KLAMATH PENEPLAIN............ 42 KwnopF, A., petrographical work by. 369 KNOXVILLE FORMATION..... 112 —, locality for palacheite . 231 Kuntz, cited on a corundiferous andesite IM) MONAT Al ceec.speeusseteess dhvctavsceaesiazesseees 221 ILACROIX, cited on magmatic resorption... 135 in Upper LAMPROPHYRE DYKES Kern Basin LANDSLIDES, Black Hills —, characteristics ....... —, discussion RESTON cesecesten sec —, Klamath Valley , Pearch Creek Valley iy ATER QUATERNARY epochs. LAURENTIAN ROCKS T@AVIASs.osscascsvecathesacense 151, 300, 374 LAwson, A. C., cited on iddingsite.......118, 162 ——,on length of Quaternary Era. . 470 ——, on marine terrace : 2 —-—, on upthrust of Montara Mountain... 6 LECONTE, J. N., cited on glaciation in Southern Sierras. 355 ——, on living glaciersin Sierra Nevadas 366 =a 7. N., barometric measurements Dyn LpowA HEIGHTS, MUMerAalS PROM a eesscrecs 191 480 LINDGREN, on redingtonite..............ccee eee 232 LITTLE KERN PLATEAU, a terrace.. LIVERMORE VALLEY, gravels at.. LOESS, origin of...... LONE PINE PEAK .Ji,.ccceccscress MACKYARUM FALLSs ... MARKUSEN MINE, large boulders in... ——) Liver terrace ....s0ssiecsserseeseace ead = LOLTONT LATIN, cessesseeexasscteece a MASCALL Brps, of John Day Basin......... feecpncenhasteee teers ese 114, 166, 238 ., cited on fossils of John MATTHEW, . Day Beds... MCADIE, A. G., cited on heavy precipita- LLOLIS GE SO 7 OSes tess eeeeee ess — —, barometric measurements b MELLENIA SERIES ...........cseeeeeseeees MELVILLE, cited on redingtonite.............. 232 MERRIAM, J. C., cited on basalt of Blue Mountain Range.... 114 — —-—, columnar structure of tuff beds ... 149 — — —, fossils of John Day Beds — ——-; John Day Basini:.s.:..... — — —, modification of tuft beds .... — — —, expedition to John Day Basin...... METAMORPHIC Rocks of Orleans Region.. 42 ——, of Sierra Nevada Region f...:.0s1.c0. 298 MICA-AUGITE-ANDESITE, corundiferous .., 221 MICROLITEG........ MIDDLE Fork glacier .... MIGRATION of flora of Klamath Region ... 464 MILLER, W.E., cited on corundum—bear- ANS SrOCK Sar eer en see en iieecses 220 MINERAL KING belt of metamorphic MOCKSHA srsit assesses caetoncenavere cet 298, 362 MINERALS: —, Alunogen —, Apatite. —, Augite.. —, Biotite —, Boothite, chemical properties — —, crystallographic characters ——==, peneral descriptiow’ <.....-.. ——., physical properties —, BY tOwWNitera.s.csuntees weal oite —, Chaleanthite, chemical proper -— —, crystallographic characters... ——, general description a.....1 —, Chalcedony.... —, Chalcopyrite..... == CMILOLItGs erect cree 83 —, Colemanite 406 —, Copiapite, chemical properties. 214 — —) general description :c:..ereere.-,: » 214 =, CODPehan sce. Bs - 195 —, Coquimbit 32) —, Corundum. 226 —, Edenite... 225 — Pesta titewscccactsiseeress 120 —, Epidote ..: 388 —yPSOMMICE: atin, seneeesdesesssecdscscsess 3 232 —, Feldspar..:.. 178 a= SELCIN ALLE hy, ccc xcaseissaveresececsed see aveeseen 217 —, Heulandite ... es, SL = EA eta tewacessseeere sevatere sees: a 275 ma PLOT DICH CGS cass. rcce star 131, 177, 267, 370, 386 University of California. MINERALS: Page —, Hypersthene 124, 386 —, Iddingsite... -118, 125, 131, 162 —, Umienite .2..,..:...000-.2 ee 386 ey PLLO Le reas «= 386 —, Knoxvillite —, Kunzite..... . ponnaaciie 7s —, Labradorite..... - 178, 374, 376 —) WEpidolite ieeric.sscta sts ee cee eee 266 —, Limonite.. 192, 217 —, Magnetite. 178, 370 —, Marcasite e232 —, Melanterite, chemical properties.. — —, crystallographic characters.. — —, general description ...... — —, physical properties —, Muscovite —, Oligoclase —, Oligoclase—andesine . —, Olivine... — OMA sca. = 'Orthoclase,...2.:.c0..ssrceteee ee 267, 369, 372 —, Palacheite, chemical properties........... ——, crystallographic characters . = OCCULLGN CGE sen eee — —, physical properties ..... —, Pisanite, chemical properties .. — —, crystallographic characters ==, general description sy... — —, physical properties —prlacioclases ss sas. —, Pyrite, chemical properties . ——, crystallographic characters — —, general description.......... eV LOREN Cases sateeee —, Pyrrhotite ... ==, QUATUZ screens: —, Redingtonite . —, Rubellite.... —, Rubrite , Rutile. , Serpentine. —, Sillimanite Spinel ........ Spodumene . Titanite... —, Tourmaline.. —, Tridymite .. MINT CANON MIOCENE of Contra Costa County....... MODERN ALLUVIUM ... eae Soe EUDOGH ay esresseerers cst 723) — tilting of river terraces near Newhall... 25 MOHAVE DESERT, age of detrital slopes... 23 —, Late Pliocene condition of.. en MORAINES above mouth of KeenneRivet:sscoecdsssctaiesersteun reece —, lateral of Cliff Creek Valley ——, of Little Kern Cafion -.. — —, of Rock Creek Valley... ——, of Whitney Creek Valley. =~ Tlear Coyote Creek........55 — of Upper Kern Basin 9345 MoROZEwIcz, cited on corundum-bearing TOCK Si, ence lespacecritsieseneetuaneth a ee 220 MURPHYS, Quaternary gravels at........c.e.. 277 NEWBERRY, J. S., cited on red color of formations 20.0.0 463 NORIAN SERIES.. # INORITEN cos suipissssesserseect ete ee Index to Volume 3. OGISHKE CONGLOMERATE . OLIVINE NORITE vecnccneccnsees ORLEANS BASIN, described —, estimated age of terraces in —, Modern canon m= Tver LELLACES cccssarcns —, 45-foot terrace . —, 70-foot terrace... — — —, 120-foot terrace —, 475-foot terrace. —, 675-foot terrace. —, 850-foot terrace — Mountain .... OROGRAPHIC disturbance, Early Quarter- DLAI Wirieeere aise cent ormeas tse teerrenensceecesecr dass 3 OsBoRN, H. F., cited on Diaplosauria ...... 420 OWL MINE gravel deposit ...........cceereees 430 PAJARO, igneous rocks near. 2 173 PALA, locality for spodumene 265 PARIS CANON fossil locality.. 397 PEARCH CREEK gravel deposit 449 — Mine gravel ecpos 437 — —, torrent fan at.. 437 PELONA SCHISTS.. 2 PENFIELD, 5. L,., cited on ‘spodumene 274 PEGMATITE é 297 , bearing spodumene 266 PENHALLOW, D. P., fossil wood studied by gocavie paEeprenes ++ 439, 441, 464 PENEPLAIN of $ outhern Sierra Region 363 PENOKEE SERIES ....... 58 PERIDOTITE near Span 222 PERLITIC structure jay PIEDMONT glacier near Milestone Moun- CED OD eerremeeee 354 PIRSSON, cited on 1 lamprophyre dy k 221 Prru CaANon 9 PISANI, cited on pisinite 205 PLATEAUX obliterated by cirque SEPP ius: 361 PLEISTOCENE PERIOD, epochs of... 28 —, erosion in Klamath Region 471 PLIOCENE PERIOD, limit of .... i PLUMASITE, chemical composition 227 —, correlation . 229 ae discovery Scat 221 excell, 225 —, near Spanish Peak . 219 Post-GLACIAL degradation of Kern RESTON ereaesseee sausidaseseaasicqnarerscssemenetioete 300 POTTER CREEK cave. 412 Pratt, J. H., cited on ‘corundiferous 220 PYROXENITE.., 18 CUS TEENS lavas of BREESE Kern Basin Perret re arr ory ..300, 374 , length One, 367 — of John Day Bas 115 =p Sotthern: California pes.ccse esses RANSOME, cited on an augite-latite flow.... 243 RATTLESNAKE CREEK... —, Formation .. —, Gravels of John Day Basin. 238 RAVENNA PLUTONICS 2 RED BLUFF EPoOcH ... II — — Formation, age of.. 12 —— Terrace of Sacramento Valley REDNECK ROCK.. Side Hetres ceesa males RED SPUR MOUNTAIN ee REMSEN, I., cited on melanterite. REPOSSI, E., cited on Wivosaurus ... REVERSED drainage in Toowa Valle 328 RHYOLITE.. 7122),137,, T41,)152) 156). 168, 772 RIVER terraces in Southern California ...... ro 481 age ROARIN GukunVvik Ricsue.cteacensen: ts teeeenranarenihtirraia OO ROCHES MONTONNEES .........+ 350, 352, 452 ROCK CREEK.. Sastre eTLo) — — glacier.. » 350 ROCK-SLIDES of Kern Cajion. 343 RODGERS DRY LAKE. 20 Roor of granite in Upper ‘Kern ‘Basin 301 ROSAMOND SERIES 2 ROSENBUSCH, cited on corundum 219 RUSSELL, I. C., on red color of certain FOTMIATIONUS i tasssssacetarteniessivstseesaseeress ce AOS, SALSTROM MINE, river terrace at.............. 440 — — torrent fan SAMWEL CAVE SANDY BAR terrace SAN EMEDIO schists — Pedran Epoch.. — Pedro Hill terrac , correlated... SANTA CLARAN EPoc! A74 — Clara River terrac A74 ScoTt VALLEY, aggraded. 72 SHALER, N.S., cited on detrital slopes. 21 ——,on Mohave Desert . 4 HASTASAURUS, affinities... 85 —, characteristics. —, classification —, distribution , synonomy . SHEEP MOUNTAID SHELTON BUTTE .. FF, SHERWOOD VALLEY of Klamath River..425, 470 SIBERIAN Outpost, plateau near 308, 316 SIERRAN CANON of Klamath River — Period river terrace cited on Tria SIMS GULCH, SMITH, J. P., County —, W.S. T.. on marine terraces. Sor, change of color of. SOLEDAD CANON 10, 19 "PASS ve scanstsee cere s se ctacstudenedssdeeseeseaceecizetes 19 SOUTHERN CALIFORNIA, sketch map of... 2 SPANISH PEAK, plumasite locality SPHERULITES .... SPIRIFERINA BEDs _, chemical composition . —, etch figures. —, forms.......... , found near Pala, Cala , habit — phy sical properties. st. JOHN, O., cited on fossil fish SUB SUMMIT PLATEAU of Region ——_—, sivnificance Ones festive SUMMERVILLE BASIN, terraces of ........... SUMMIT UPLAND of Sierra Nevada Region Upper 308, 710, 364 TABLE Mountain, a Summit upland TONING ooo cscccastzeceisneissecass casseeers snore 309 TALUS IN KERN CANO 358 TAR in fossil egg saan 4OZ TENNESSEE FLAT river terrace................. 432 TILTING of ancient valleys in Kern Kegion.. 327 , terraces in Orleans Basin 461 TOOWA VALLEY. 300, 319, 365 ——, lavas......... 300 ——, mature topography . 322 ILO HA COG a aitinneenaraslasecuee sic se ceransacass aha ees 322 482 Page TOOWA VALLEY, volcanoes.............0008 320, 366 ‘TOPOGRAPHY controlled by structure, Kenn ReSiO1s scenes — —— —, Klainath Region . TORRENT FANS of Orleans Bas cance of TORTOISE, fossil from Auriferous Gravels TOWER Rock, +305, 340 ime- 300 424 nifi- SUOM GC: ec sscecd sous docs iivcsavevansesascccsastessbaaeees Tracuytic tuffs of John Day Basin... ‘TRAVERTINE.. TRIBUTARY giaci TRINITY SUMMIT . ‘TROCTOLITE — —, determined by a rift line . TRUNK GLACIER in Kern Cafion — — —, terminal moraines of.... Tuff. evogh cacesstaisseasss vivases T3, 133, 145, 145, 100, 272. AyeDeC Si cesses 149 TURNER, H. W., cited on glaciation of era N@Vadas weeeecesscssscssessvsessseeseeees 2 os —-, SSCLDCILING. 2 aireiaeceeisesseteesterssscaacs 222 ——, soda syenite near Meadow Valley 229 ‘TYNDALL CREEK .. a UNDERGROUND Channels in limestone ..... 300 UPLIFT, axis of, in Klamath Region ........ 471 UPPER KERN BASIN, cirques of. 357 — — —, crustal rifting in.. 3 ———, diagram mC — — —, drainage . 305 —— —, general relief. 305 —— —, geomorphogeny of. , 306 ———, glaciation ... 345 — ——, granitic rocks. nies Preaek) — —'——, JOIN TA GEA ascsssesunsad siesta sisee sieves 302 University of California. UpreER KERN BASIN, petrography. — — —, structural features ............ — — —, studied by Gilbert and Lawson ... 292 ——, Cafion. —-—, Lake .. — — —, due to debris — Marquette Series — Menominee Seri — Pliocene Strata in Los Angeles County 3 —-San Pedro!Series:..ci.c...cscsteocseseccremeentens 27 cones VALLECITO, fossile tortoise found near ..... 243 VANDEVER MrT., high plateau west of. 309, 314 VAN HIsE, C. H, cited on Algonkian ...... 61 VOGESITE 372 VOLCANO CREEK.. . 320 VOM RATH, G., cited on colemanite or 32 WASHINGTON, cited on Italian lavas ........ 126 WATER COURSES, absence of, in upland of Kern Region eats WEBSTERITE. = (15 WEITCHPEC, high floods at - 459 WHITNEY CREEK. . 306 — — glacier 351 — Mount . 3 + 302, 352 ; Ji-nD:; cited on Miocene andstones...... 379 WILDER DiGGInGs landslide deposit ........ 443 — —, river terrace re 2 — Ferry, river terrace near . 430 — Mine, fossil wood . . 441 WiLLmorr, cited on Algonkian ar 61 — — —, correlation in Lake Huron Region 59 WOODWARD, A. S., cited on fossil fish ...... 400 WORTHEN, A. H., on fossil fish . 400 YOSEMITE VALLEY, glaciation of............ » 359 ZEPHAROVICH, cited on melanterite......... 197 te, e * — me yore AX 7. Minerals from Leona Hetehiee Alameda Co., aol ane By, Waldemar T. — . The Quaternary of Southern California, by Oscar H. Hershey . Colemanite from Southern California, by Arthur $, Eakle . The Eparchzean Interval. A criticism of the use of the term Algo . Plumasite, an Oupdelsce -Corundum Rock, near ‘Spanish Peak, California, 3 % . Palacheite, by Arthur S. Eakle ; F : “Price, ToC as . Two New Species of Fossil Turtles from Renn < On. “Hay In one . A New Tortoise from the Auriferous Gravels of. California, by >} cover, W. J. Sinclair Price, ube . New Aa place Ta from the TBP Triassic of California, Oy ome C. Merriam ~ : Becanhor from San Brees Co., California, by Waldemar T. Schaller Price, To . The Pliocene and Quaternary Canidae of the Great rae of California, . The Geomorphogeny of the Upper Kern Basin, ou Andrew C. Lawson Price, 6 . A Note on the Fauna of the Lower Miocene in California, by John iC . The Orbicular Gabbro at Dehesa, San Diego Co., California, by AndrewC. 9 . A New Cestraciont t Spine from the Lower Triassic of Idaho, Herbert M. . A Fossil Egg from Arizona, by Wm. Conger Morgan oe Marion Clover . Euceratherium, a New tik siege from the Quaternary Capes of. California, . A New Marine Rea from the Triassic of ase by joe C. Merriam. : The River Omesiies of the Orleans Basin, California, = Oscar H. Hershey. VOLUME 3. by Andrew C. Lawson Triassic lchehyonenyer from California ea Nevada, i Jot C. Merriam © DIABE, . A Contribution to dhe Petrography of the John pe. Basin, by Praale Cx : Calkins ; ; Price, . The Igneous Rocks near Pajaro, by ae A. Reid : f ~ .. “Priee; tg Schaller. ‘ . > Prige aie. by Andrew C, Lawson at gears” eel . , Se Bie ators file Price, by John C. Merriam . : Price, Merriam : : Price, aoe ‘ Lawson : % Price, 10c se Evans . r -* APrice; se Tallmon " tae : Price, roc’ > by William J. Sinelair and E. L. Furlong 5 : ; : Price, » TOC Price, pee , : Price, 35° INOUE II 3 9088 01308 9818