LIBRARY OF THE UNIVERSITY OF CALIFORNIA. GIFT OF Class 30% UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 4, No. 13, pp. 263-286, Pis. 31-37 ANDREW C. LAWSON, Editor COLD WATER BELT ALONG THE WEST COAST OF THE UNITED STATES BY RULIFF S. HOLWAY BERKELEY THE UNIVERSITY PRHSS November, 1905 PRICE 25 CENTS The BULLETIN OF THE DEPARTMENT OF GEOLOGY of the University of California is issued at irregular intervals in the form of separate papers or memoirs, each embodying the results of re- search by some competent investigator in geological science. These are made up into volumes of from 400 to 500 pages. The pricf per volume is $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 PRESS, to which remittances should be addressed: VOLUME 1. PRICE 1. The Geology of Carmelo Bay, by Andrew C. Lawson, with chemical analyses and coop- eration in the field, by Juan de la C. Posada 25c 2. The Soda-Rhyolite North of Berkeley, by Charles Palache lOc 3. The Eruptive Rocks of Point Bonita, by F. Leslie Ransome 40c 4. The Post-Pliocene Diastrophism of the Coast of Southern California, by Andrew C. Lawson 40c 5. The Lherzolite-Serpentine and Associated Rocks of the Potrero. San Francisco, by ~\ r Charles Palache / In one 6. On a Rock, from the Vicinity of Berkeley, containing a New Soda Amphibole, by t cov f r - Charles Palache . . . . . . . ) 30c 7. The Geology of Angel Island, fry 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 . . . 45c 8. The Geomorphogeny of the Coast of Northern California, by Andrew C. Lawson . . 30c 9. On Analcite Diabase from San Louis Obispo County, California, by Harold W. Fairbanks 25c 10. On Lawsonite, a New Rock-forming Mineral from the Tiburon Peninsula, Marin County, California, by F. Leslie Ransome lOc 11. Critical Periods in the History of the Earth by Joseph LeConte 20c 12. On Malignite, a Family of Basic, Plutonic, Orthoelase Rocks, Rich in Alkalies and _ Lime, Intrusive in the Coutchiching Schists of Poohbah Lake, by Andrew C. Lawson . 20c 13. Sigmogomphius LeContei, a New Castoroid Rodent, from the Pliocene, near Berkeley, by John C. Merriam 10c 14. The Great Valley of California, a Criticism of the Theory of Isostasy, by F. Leslie Ransome * 45c VOLUME 2. 1. The Geology of Point Sal, by Harold W. Fairbanks 65c 2. On Some Pliocene Ostracoda from near Berkeley, by Frederick Chapman . . . 10c 3. Note on Two Tertiary Faunas from the Rocks of the Southern Coast of Vancouver Island, by J. C. Merriam 10c 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 .... lOc 5. The Geology of Point Reyes Peninsula, by F. M. Anderson 25c 6. Some Aspects of Erosion in Relation to the Theory of the Peneplain, by W. S. Tangier Smith ... 20c 7. A Topographic Study of the Islands of Southern California, by W. S. Tangier Smith 40c 8. The Geology of the Central Portion of the Isthmus of Panama, by Oscar H. Hershey 30c 9. A Contribution to the Geology of the John Day Basin, by John C. Merriam . . . 35c 10. Mineralogical Notes, by Arthur S. Eakle lOc 11. Contributions to the Mineralogy of California, by Walter C. Blasdale ... . 15c 12. The Berkeley Hills. A Detail of Coast Range Geology, by Andrew C. Lawson and Charles Palache " 80c VOLUME 3. 1. The Quaternary of Southern California, by Oscar H. Hershey 20c 2. Colemanite from Southern California, by A rthur S. Eakle 15c 3. The Eparehaean Interval. A Criticism of the use of the term Algonkian, by Andrew C. Lawson . lOc 4. Triassic Ichthyopterygia from California and Nevada, by John C. Merriam . . 50c 5. A Contribution to the Petrography of the John Day Basin, by Frank C. Calkins . 45c 6. The Igneous Rocks near Pajaro, by John A. Reid 15e 7. Minerals from Leona Heights, Alameda Co., California, by Waldemar T. Schaller 15c 8. Plumasite, an Oligoclase-Corundum Rock, near Spanish Peak, California, by Andrew C. Lawson "... lOc 9. Palaeheite, by Arthur S. Eakle lOc 10. Two New Species of Fossil Turtles from Oregon, by O. P. Hay . . 1 In one cover. 11. A New Tortoise from the Auriferous Gravels of California, by W. J. Sinclair / lOc 1 "2. New Ichthyosauria from the Upper Triassic of California, by John C. Merriam . . 20c 13. Spodumene from San Diego County, California, by Waldemar T. Schaller . . . lOc 14. The Pliocene and Quaternary Canidae of the Great Valley of California, by John C. Merriam 15c 15. The Geomorphogeny of the Upper Kern Basin, by Andrew C. Lawson .... 6oc 16. A Note on the Fauna of the Lower Miocene in California, by John C. Merriam . . 05c 17. The Orbicular Gabbro at Dehesa, San Diego County, California, by Andrew C. Lawson lOc 18. A New Cestraciont Spine from the Lower Triassic of Idaho, by Herbert M. Evans . lOc 19. A Fossil Egg from Arizona, by Wm. Conger Morgan and Marion Clover Tallmon . . lOc 20. Euceratheriunv a New Ungulate from the Quaternary Caves of California, by William J. Sinclair and E. L. Furlong lOc 21. A New Marine Reptile from the Triassic of California, by John C. Merriam . . 05c 22. The River Terraces of the Orleans Basin, California, by Oscar H. Hershey . . . 35c OF THE " UNIVERSITY ) OF UNIVERSITY OF CALIFORNIA PUBLICATIONS BULLETIN OF THE DEPARTMENT OF GEOLOGY Vol. 4, No. 13, pp. 263-286, Pis. 31-37 ANDREW c. LAWSON, Editor COLD WATER BELT ALONG THE WEST COAST OF THE UNITED STATES BY RULIFF S. HOLWAY CONTENTS. PAGE Introduction .................................................... 263 Temperature Observations of the Tuscarora ....................... 266 Temperature Observations of the Albatross ....................... 269 Inshore Belt of Cold Water .............................. , ....... 271 Two Problems Presented ......................................... 274 Cold Water along Other Coasts ................................... 274 General Temperature Conditions of the North Pacific ................ 277 Maximum Surface Temperatures ............................... 278 Minimum Surface Temperatures ............................... 278 Eange of Surface Temperatures ................................ 278 Temperature of Ocean Bottom ............................ 279 Hypothesis accounting for Cold Water Belt ........................ 281 Summary ................................... ogg INTRODUCTION. Although considerable attention has been paid to the question of ocean currents off the west coast of the United States, yet much work remains to be done, that accurate information as to the limits, direction and temperature during the year of the various streams or drifts may be ascertained. The Pilot Charts of the North Pacific, issued monthly by the United States Hydro- graphic Office, give for each of the four seasons a somewhat schematic current chart which is virtually a composite of the observations received by that office. Upon the face of each sheet there is a statement printed in red, calling attention to the 172922 264 University of California Publications. [GEOLOGY meager data upon which the currents are charted. In the preparation of the Pilot Charts, only actual reports by officers crusing in the Pacific are considered and particular attention in observing and reporting currents is requested of all mariners. The amount of current reported by a vessel is the difference in the position of the vessel each day as obtained by dead reckon- ing and the position obtained by astronomical observation. In getting the position by dead reckoning, there are several sources of error. Among these are the variation of the log in finding the velocity of the ship, the failure of the man at the wheel to hold the ship accurately to the prescribed course, and the un- certainty as to the exact variation of the magnetic needle. This last source of error may be of considerable amount. The North Pacific Pilot Chart for February 1904 says: "Taking the whole of the navigable world into consideration, it would be conservative to state that the general uncertainty in the heading of a ship at sea, arising from an inaccurate knowledge of the variation of the needle, is as much as two degrees. ' ' This alone would make a discrepancy of 15 to 20 miles between the calcu- lated and the true position of a fast steamer at the end of each day's run. Turning to the other half of the problem, it is found that a probable error of 2% miles must be allowed in obtaining the true position by astronomical observation.* The difference between the ship's position as determined by these two methods with the possible sources of error is reported as current or drift. It is well to note that the reports of steamers have not the same value as those of sailing vessels. The sailing vessel is occasionally becalmed for an entire day and then the difference in position between two astronomical observations gives a reasonably accurate determination of the drift. The normal rate of a ship being known, it would seem as if it might fully be allowed for, and hence the current might be determined from a vessel under way, with an equal accuracy as from a drifting ship. This would be true were it not for the fact that ocean currents and drifts are not large masses of uniformly moving water, but rather relatively narrow streams with bands * Estimate by Professor George Davidson. VOL. 4] Holwaij.Cold Water Belt. 265 of calm water or even counter eddies between. A steamer mov- ing rapidly may pass through several narrow streams of differ- ing velocity or even differing direction and its report of current would then be the algebraic sum of the various currents en- countered. A becalmed ship or even a slow-moving sailing- ship is apt to remain in one stream for the entire 24 hours. This is supposed to account for some of the widely differing reports of sailing vessels and of steamers in traversing the same region. With the increasing commerce of the Pacific the num- ber of reports from both steamers and sailing vessels will in- crease, and reasonably correct information will be obtained for the zones traversed by regular vessels. For the parts of the ocean out of the usual courses laid down, reliance must be placed in the scientific expeditions devoted to oceanic research. An important addition to the reports of currents encoun- tered by vessels are the so-called "bottle tracks." Bottles usually made of rubber are thrown overboard with an inclosed slip giving the latitude and longitude of the ship at the time. On the bottles is a printed request that they at once be returned to the authority conducting the investigation, with a statement of the time and place of finding. The bottle track is the line connecting the place of starting and the place where found. A minimum rate of drift is thus established. The line of drift and the time that the bottle may be stranded on some coast before being found are the elements of uncertainty. If the bottle is so weighted as to expose practically no surface to the wind, its movement depends entirely on current or drift and "bottle tracks" thus form a valuable element in current deter- mination. A third important source of information is found in the constantly growing mass of data on ocean temperatures. The thermometer is one of the most reliable instruments in deter- mining currents. Unfortunately much of the data for ocean temperatures on this coast is scattered through the reports on file in the Hydrographic Office and is not accessible to the public. It is to be hoped that more of this will be tabulated and made available to investigators as has been done by Mr. C. 266 University of California Publications. [GEOLOGY H. Townsend* for the work of the Albatross for the years 1883- 1900. The original observations upon which this paper is based are found largely in Mr. Townsend 's compilation and in the valuable work of Admiral Makarofff which tabulates tempera- tures taken in the North Pacific from 1804 to 1890, but does not include the work of the Albatross. TEMPERATURE OBSERVATIONS OP THE TUSCARORA. J Some of the most marked peculiarities in the temperature distribution off the west coast of the United States are well shown by tabulating the observations of Commander Belknap of the U. S. S. Tuscarora. In 1873 the Tuscarora had been de- tailed for the purpose of finding a suitable route for a cable between the United States and Japan. A series of soundings was made on lines running west from the Pacific Coast to deter- mine the slope and the general nature of the ocean bottom near shore. Incidentally the temperature of the ocean water was taken the series of observations is fairly complete for surface and bottom temperatures but rather incomplete for serial tem- peratures showing the conditions at intermediate depths. The surface temperatures obtained on 14 lines running approxi- mately west from the coast and at intervals from Cape Flattery to San Diego are given in the table herewith. The first tem- perature in each line is the temperature found nearest shore. Unfortunately this is not at a constant distance from the coast line. Where the difference is material, the first sounding is set o\er a corresponding amount in the table. The first line of soundings was made September 17 to 20, 1873 ; the eight lines from Flattery Rocks to San Francisco, Oc- tober 20 to November 6 ; the lines between San Francisco and San Diego from December 20 to 30. As these observations were distributed over a period of three months, each line of soundings must be taken by itself to avoid confusing seasonal * U. S. Fish Commission, Eeport for 1900, pp. 387-562. t Makaroff, S. Le Vitiaz et L 'Ocean Pacifique, St. Petersburg, 1894. j Belknap, Geo. E., Deep Sea Soundings in the North Pacific. U. S. Hydrographic Office, 1874. Found also in Makaroff 's work. CO p p San Nicholas 3 CO E- 1 f 5. 5 Pt. Carmel San Francisco CO Si 2. B p C. Mendoeino Trinidad Head M B V 8 o e* ^ C. Foulweather Flattery Eocks p CD" 3 Shore end of line co to CO CO CO CO CO to CO h^ Oi CO CO Ol 1 1 Ol CO OS to Ol CO o CO GO CO CO CO o 00 o CO Ol to *- GO Ol First 5 Latitude r to 00 CO Ol CO to o to Ol GO to to o ^ IO CO CO OS to CO OS to o to i CO o to s to to Ol to 4^ to to to Ol _ ^ to P Qj " a a a e o C5 " -. o 3 a a O rl- CO h-i CD GO rt- CO 99 CD 1/1 CD 00 Ol h-" Ol CO Ol b Ol Ol to bo co OS GO bi Ol CO to Ol o Ol O Ol CO os Ol Ol b Ol Ol b Ol to bo Ol Ol os co Ol to Ol bo Ol 01 io Ol Ol b Ol Ol bi Ol Ol b Ol CO h- 1 Ol OS Ol o to Ol to co Ol CO to Ol co b Ol os *. Ol o Ol Ol b Ol Ol bo Ol CO CO Ol O3 bi O 01 O Ol OS b Ol Ol b Ol b Ol CO to Ol to b Ol co b Ol OS bo Ol to h- ' Ol OS Ol b Ol Ol CO bo Ol cc Ol Ol b Ol Ol co b Ol Ol OS Ol h- b Oi b Ol b Ol b Ol GC to Ol 00 b Ol H o B Ol 00 b 9 si Ol co 03 Ol OS Ol to Oi CO b Ol -q 05 Ol b Ol GO Q Ol GO bi gj cr Ol GO b Ol P bi g bo O o OS CO o CO CO OS 02 o CO o to O o OS co o o Oi o to o o CO co- o Ol o to -. h- ' o o CO h- ' O ( * z; Northing or Southing O Sj a > rO ^ hd > rr H m S CO H o d a w Q w He) O S3 g S > ^1 |i hr| W IT ^ W ^ GO _ w 1267] 268 University of California Publications. [GEOLOGY changes to changes due to differences in latitude or to distance from the coast line. In the published records of the observa- tions we are not given the time of the day nor the condition of the weather. According to Buchan's discussion of the Chal- lenger observation, the daily variation of the temperature of the surface of the sea does not exceed 1 F. In general the differences considered in this paper greatly exceed that amount. The first line of temperatures in the table is but a part of a survey extending from Cape Flattery nearly to Dutch Harbor on the island of Unalaska, made during the latter part of Sep- tember, 1873. The first temperature near shore was 50.4. In going westward 120 miles and northward about 40 miles, the temperature increased to 59. From this point the rest of the survey shows a gradually falling temperature, but the initial temperature of 50 was not again reached until the vessel was nearly 1,000 miles to the westward, about 370 miles north of the starting point and only some 200 miles from the island of Kadiak on the Alaska Coast. This increase of temperature on first leaving the coast and the subsequent slow decrease are more striking when it is con- sidered that the last records were made two weeks later in the autumn than the first. The next eight lines of survey represented in the table ex- tend off shore from 100 to 200 miles. Their lengths are shown approximately in the table where each column represents 15' of longitude. These lines uniformly indicate that the water near shore is colder than that further to the westward along the entire coast from the Straits of Fuca to San Francisco. The lowest temperatures obtained are at Cape Mendocino and Trinidad Head and are at the two stations which are the closest inshore. They are also near the change to the southeast in the direction of the coast line. It is noteworthy that these lowest temperatures are not those found further north. On the con- trary, according to the data now at hand, it is more than 500 miles to the northward before surface water as cold as that near the coast between Cape Blanco and Cape Mendocino is reached, during the late summer and the early fall. VOL. 4] Holway.Cold Water Belt. 269 Southward of San Francisco the temperatures in the table do not show such marked variations. The first three lines all north of Point Conception are in harmony with the existence of an inshore belt of cold water. South of Point Conception there is no evidence of such a cold belt. As indicated in the table the length of the lines south of San Francisco is less than that of those to the north. The Point Sal and the San Nicolas lines also vary greatly from east and west lines. South of Point Conception, the submarine plateau or con- tinental shelf is much wider; that is, there is a much broader area of comparatively shallow water. This wider continental plateau and the bend in the coast line at Point Conception are probable elements in the causes which determine the absence of a marked inshore belt of cold water off southern California. The temperatures in the table with those obtained by the Tuscarora in the cable survey from San Diego to Honolulu have been laid off on the coast survey charts; the cable survey tem- peratures, like the others already considered, give no indication of a cold belt near shore, south of Point Conception. For the first 150 miles from San Diego, the surface temperatures vary from 58 to 59. Beyond that, the temperature slowly rises as the line runs to the west-southwestward to the Hawaiian Islands. TEMPERATURE OBSERVATIONS OF THE ALBATROSS. In 1891-2 two surveys were made by the U. S. S. Albatross, between Monterey Bay and Honolulu the one on a great circle, the other on a rhumb line. On the great circle line, the surface temperatures for the first 150 miles vary from 54 to 56. It then rises to 59, drops to 57, and rises to 62. After that it rises slowly as the line runs toward the tropics. The observa- tions on the Monterey end of the survey were made in October, 1891. On the rhumb line in January, 1892, the temperature off Monterey Bay was 52, rising to 59 in 140 miles. Even with a liberal allowance for the southing made on these lines, the surface temperatures near shore are distinctly lower than further to the westward. 270 University of California Publications. [GEOLOGY The vertical distribution of temperature ( on these two lines is shown on the isobathymetrical charts accompanying the re- port of the survey.* In both cases' the isobathytherms in the upper part of the ocean rise on approaching the California Coast. They indicate that water near the surface close inshore is as cold as that 1,000 to 2,000 feet below the surface 200 to 400 miles off shore. From 1888 to 1900 the Albatross made several series of hydrographic soundings along the Pacific Coast. A line run in September, 1888, off Cape Flattery falls between the first two lines in the table of Tuscarora soundings. The stations are close together and the temperature rises from 52 to 61 in run- ning off shore about 50 miles and in the next 30 miles falls, but only to 59. The inshore cold belt is well marked, for the temperature remains at 52 for the first 20 miles. Southward from Cape Flattery to Cape Mendocino the series of surface temperatures is quite complete but they are usually confined to a coast belt of less than 30 miles in width. They are also scat- tered through various months in the term of 12 years. For comparison with the Tuscarora observations, temperatures taken during the autumn months have been used. The general result has been to confirm fully the conclusion that a belt of cold sur- face water exists near shore. Of equal interest is the fact that the temperatures show narrow belts of warm and of cold water lying close together and frequently occurring in the area cov- ered in one day's observations. Usually these narrow belts are at right angles to the coast. This peculiar arrangement of the minor temperature belts seems to negative definitely the idea that the cold coast water is due to an inshore Arctic current, for such a current would give a stream of moderately uniform surface temperature and the variations that did occur would naturally extend in belts or lanes having the same longitudinal direction as the main stream. As an illustration of the results obtained in charting these temperatures, a section of the coast extending about 150 miles northwest from Cape Blanco is shown in PL 31. Close inshore * Senate Ex. Doc. No. 153, 52nd Cong., 1st Ses. BULL DEPT, GEOL. UNIV, CAL. VOL. 4, PL. 31 Surface temperatures along a portion of the Oregon Coast for August or September. The 100-fathom line and an occasional deep-water sounding indicate approximately the ocean depths. The dotted lines connect tempera- ture observations made on the same day. VOL. 4] Holway.Cold Water Belt. 271 the temperatures ran from 47 to 52 in the vicinity of Coos Bay from September 10 to 12/1889, while on the llth a little further off shore there is a short line running from 57 to 59. Notice also that on the same day within 10 miles on the north and on the south, there are lines with temperatures varying from 50 to 54 ; that is, of the three short lines at right angles to the coast just south of Coos Bay, the middle line averages about 6 warmer than the other lines. Over the Heceta Bank, it will be noticed that temperatures of from 60 to 63 occur, while close inshore a temperature of 49 occurs only ten days later. The ten days' difference in time can cause no appre- ciable seasonal change in temperature and the variation from 63 to 49 very probably was true for the same day. The lines of temperature for August 30 and 31 are typical in showing the colder water inshore, the exceptions to this rule being few and with slight differences in temperature. No exception has been found with east or west lines of 50 to 200 miles in length and which run close inshore. INSHORE BELT OF COLD WATER. This general idea of a cold inshore belt has long been recog- nized. Richter* discussed the Tuscarora temperatures and called attention to the belt of cold coast water which they indi- cate. Apparently without other observations he accounted for the presence of this cold water by assuming the existence of a cold surface current from the Arctic. Part of Richter 's argu- ment is based on the strange error that "the western coast, of the United States trends northeastward from Cape Mendocino to Tatoosh Island, ' ' when in fact Tatoosh Island is slightly west of north from Cape Mendocino. As already stated, a study of the temperature relations found in PL 31 renders highly im- probable this idea of a cold polar surface current. Before dis- cussing the hypothesis advanced in the present paper to account for the cold inshore belt, the temperatures for greater areas of the North Pacific should be examined. The temperature charts * Eichter, C. M. Ocean Currents Contiguous to the Coast of California. Bull. Cal. Acad. Sei., vol. 2, p. 337. 272 University of California Publications. [GEOLOGY for the entire west coast give a mass of detail which can be studied best by expressing the figures for a limited period by isothermal lines. In PL 32 is given- the general result for the month of August. A salient feature of this chart is the area indicating warmer water to the north of the inshore belt of cold water as well as to the west and south. The fact of the presence of this warmer water in addition to the minor belts of varying temperature already shown in PL 31 seems to exclude entirely the hypothesis of a cold, polar surface current along the west coast of North America. The only remaining explanation is that there exists a belt of cold water upwelling from the adjacent ocean depths. Possible reasons for this upwelling will be discussed later. A prior consideration is the general trustworthiness and the de- gree of accuracy of the isotherm in PL 32. The writer feels con- fident that the location of the coldest part of the inshore belt in the vicinity of Cape Blanco and Cape Mendocino and the exist- ence of warmer water to the northward are fully established. The exact position of the isotherms is open to doubt but it is not believed that the error is sufficient to affect the general relations which can be shown on a map of the scale used in PI. 32. More- over the problems and conclusions of the paper will not be changed by a future shifting of the boundaries of the tempera- ture zones here represented. The essential differences between the chart here presented and previous isothermal charts of the North Pacific for the month of August will now be examined. The charts to be cited show little if any variation in the location of the isotherms in mid-ocean, but differ widely in the vicinity of the American Coast. Marakoff in his work already quoted makes the isotherm of 18 C. turn abruptly to the southward at about latitude 45 and again bend to meet the coast in about latitude 36. He thus represents the cold belt along the coast as merely an extension of the cold zone of the extreme North Pacific. The British \dmiralty charts (1886) show the isotherm of 60 C as almost touching the coast near the mouth of the Columbia River and then as swinging out and southward, finally meeting the coast BULL. DEPT. GEOL, UNIV. CAL, VOL, 4, PL. 32 Isothermal chart of the eastern portion of the North Pacific for the month of August. Lines represent approximate mean temperatures for the month. OF THE DIVERSITY OF VOL. 4] Holway.Cold Water Belt. 273 somewhat north of Point Conception. In other words, accord- ing to this chart, the belt of cold coast water along California and Oregon has a very narrow connection with the cold water of the extreme North Pacific. The temperatures for the cold belt are not so low as those reported by the Albatross, but the latter were doubtless taken much closer inshore than those used by the British Admiralty. The locality shown in PL 31 just north of Cape Blanco is marked on the British Charts as having a variation exceeding 10 during the month of August. This agrees with the belts of varying temperature found by the Albatross in that vicinity and is prob- ably due to alternate bands of the surface water proper and of upwelling cold water from the ocean depths. The isotherms of the Deutsche Seewarte chart are repro- duced in PI. 33. They show similar general relations to those indicated in PL 32, but differ in making the cold inshore belt much shorter and in locating the coldest part of the belt at two widely separated places San Francisco Bay and the Straits of Fuca, the lowest temperature being shown by the isotherm of 14 C. (57 F.). The latest data available do not greatly change the average temperatures for these points as marked on the German charts. Davidson* gives the monthly averages in the Golden Gate for 12 years of daily observations. The August mean for this period is 59.2, with 57 the lowest average for any one year. Lower temperatures are reported just outside the bar. The corrections to be made in PL 33, according to the recent Albatross observations, do not consist in a revision of the tem- peratures given for the cold water areas so much as in the locat- ing of much colder areas near Cape Blanco and in more than doubling the entire length of the belt of cold coast water. The occurrence of the coldest water in the vicinity of Cape Mendocino and Cape Blanco has an important bearing on the theory to be offered to account for the belt of cold water along this coast. * Davidson, Geo. Bull. Calif. Acad. Sci., Vol. I, p. 354. 274 University of California Publications. [GEOLOGY TWO PROBLEMS PRESENTED. The temperature relations of the surface water of the North Pacific represented in PL 32 present two problems for solution. First, what is the cause of the belt of cold water along the west- ern coast of the United States? We have already seen that it must be due to an up welling of cold water from the adjacent ocean depths, but what are the causes which produce this up- welling? And secondly, why should the coldest part of this area be in the vicinity of Cape Blanco and Mendocino, instead of farther to the northward? Before attempting to answer these problems, a brief review will be made of the discussions of cold water in other portions of the world and also of the general tem- perature relations of the North Pacific. COLD WATER ALONG OTHER COASTS. In PI. 34 A is shown the belts of cold coast water as mapped by Andrees.* Berghausf gives practically the same areas omit- ting the southeast coast of Arabia. Both authors make the belt extend along the entire Pacific coast of the United States and of Lower California. Neither of them attempts any differentia- tion of the cold water area into belts or sections of different tem- perature. In the handbook accompanying Andrees 'i Atlas, these areas of cold water are attributed to a vertical current caused by winds blowing off shore and dividing the surface water to the leeward. The supposition is that the accumulation of water to leeward would cause a return drift at the bottom of the ocean and an upwelling near the shore. A discussion and indorsement of this idea is given by Murray as a preface to his study of the effect of winds on the lochs of Scotland. With such small bodies of water as the lochs, the entire surface is under the influence of wind blowing in the same direction and return surface currents are not possible. With the ocean partial compensation may be made in other ways. * Andrees. Allgemeiner Hand Atlas, 1900. fBerghaus. Atlas der Hydrographie, 1891. J Geographisches Handbuch zu Andrees Handatlas, 1899. Murray, Sir John. Effects of Winds on Distribution of Temperature, etc. Scot. Geog. Mag., 1898, p. 345. BULL. DEPT. GEOL. UNIV. CAL VOL. 4, PL. 34 A. Belts of cold coast water according to Andrees. Compare the West Coast of North America as given here with the same region in PI. 36. B. Maximum Surface Temperatures, after Sir John Murray. VOL. 4] Holway.Cold Water Belt. 275 Harm* accepts the theory that the rise of cold water along the coast is caused by the "suction effect" of winds blowing off shore. In his general discussion he incidentally remarks "that the sharp deflection of an ocean current off shore may cause a rise of cold water from below." He does not apply the latter ideas to any of the areas which he discusses, which are substan- tially those mapped by Andrees. The whole California coast is mentioned among others as if it belonged in the area of constant trade winds. Buchananf discusses this subject and gives some data for our coast. During his voyage from Valparaiso to San Francisco in 1885 he stopped at Mazatlan. He states that on getting under way from that port the surface temperature was 75.8 and "the cold water must have been close to the surface, for water taken from the wash when the steamer was going astern had a temper- ature of 72.8." Thence across the Gulf of California the tem- perature was 78 and the water a deep blue color. Approaching Cape San Lucas the temperature of the water fell to 73.4 and then to 64.4 close inshore. After passing the Cape the temper- ature rose to 66.8 as the shore was left. Thence northward to San Francisco the water grew colder, falling to 50 degrees at the entrance to the bay. The low temperature found in passing Cape San Lucas is the most important part of this account. The cold water he found on the further trip to San Francisco being on a single line parallel to the coast furnishes little basis for dis- cussion. Mr. Buchanan offers the following comment : ' ' The occurrence of these coast areas of abnormally cold water is ex- plained when we recognize that they are the windward shores of the oceans. The trade winds blow from them toward the equator and in so doing mechanically remove water, which has to be supplied from the readiest source. This source is the deep water lying off the continental coast which is supplied by the gradual drift of water from high latitudes. Hence, though the low tem- perature of the coast water is referred to as due to the cold of high latitudes, it is not supplied by a long surface current, but * Hann, Julius. Handbook of Climatology, 1903. t Buchanan, J. Y. Similarities in the Physical Geography of the Great Oceans. Pro. Boy. Geog. Soc., 1886, p. 753. 276 University of California Publications. [GEOLOGY a short vertical one. ' ' The limits of the trade wind belt off the California coast will be discussed later, but it is needless to re- mark that these limits never reach 'as far north as Cape Blanco. Mr. Buchanan, it should be noted, does not discuss the conditions on the coast north of San Francisco. Possibly the most interesting instance of cold water rising from ocean depths is found on the Somali Coast of Africa just south of Cape Guardafui. Captain Hoffmann's account of the voyage of the Mowe is becoming classic in these discussions. The course of the Mowe was northward from Zanzibar along the coast of Africa to the Gulf of Aden. The table of temperatures here- with is taken directly from Captain Hoffmann's account, chang- ing the temperatures to Fahrenheit to agree wdth the use in this OBSERVATIONS OP CAPTAIN HOFFMANN FROM "REISE S. M. KR. MOWE VON ZANZIBAR NACH ADEN"* Latitude Longitude Date Hr. Temp. Water Latitude Longitude Date Hr. 12 Temperature Water 1886 June 28 12 79?2 4 b 41' N 48 14' E JulyS 68?0 " 28 12 75.2 " 3 4 65.6 4 42' S 39 36' E " 29 12 77.7 ". 3 8 64.8 " 29 12 77.0 7 10 ;N 49 33 E " 4 12 69.8 1 58 S 41 25 E " 30 12 79.5 " 4 4 68.4 " 30 12 77.4 " 4 8 64.2 1 15 N 43 15 E July 1 12 80.4 " 4 12 66.6 " 1 12 78.1 " 4 4 66.9 2 35 N 46 24 E " 2 12 78.8 4 8 66.2 " 2 12 74.8 9 30 N 51 21 E " 5 12 68.0 4 41 N 48 14 E " 3 12 77.4 " 5 12 73.9 " 3 4 71.2 " 5 8 6. Guardafui " 3 8 68.0 11 56 N 51 05 E " 6 12 90.3 : Ann. der Hydrogr., 1888. p. 345. VOL. 4] Holway.Cold Water Belt. 277 paper. The marked fall in temperature on July 3 and 4 was accompanied by a fall in the temperature of the air and by a change in the color of the water from blue to a deep olive green. As in this locality a cold polar current is an impossibility, unless it persists directly across the equatorial region, we are forced to the conclusion that the cold water rises from the ocean depths. Captain Hoffmann reports a strong north flowing current that makes a bend to seaward at this point where the fall in temper- ature occurs. He states that the. fall in temperature seems to be related to the change in the direction of the current. Bu- chanan attributes the cold water in this instance to the southwest monsoon blowing off shore. Hann and Andrees do the same and state that the cold water disappears with the coming of the north- east monsoon. The authorities quoted, with the exception of Captain Hoff- mann, seem to be in general agreement in accepting winds blowing off shore as a sufficient explanation of cold coast water in these areas. On our coast from San Francisco to Cape Flattery, the prevailing winds blow toward the shore, as shown in the Pilot Charts. During the passage of an extratropical cyclone, the "low" of the weather map the winds may be temporarily re- versed. As to trade winds on the California coast, the Pilot Charts for 1903 show that the most northerly extension of the trades occurring in August was to Lat. 37 30'. This was only in mid-ocean nearly 1,000 miles to the westward of San Francisco. Nearer the coast the northern limit of the trades is further to the south. At all seasons of the year the Pilot Charts show a belt of northwest winds between the Southern California Coast and the trade winds. Along Southern California where the trades blowing off shore are the nearest to the coast is the very locality that fails to show a definite belt of cold coast water. GENERAL TEMPERATURE CONDITIONS OF THE NORTH PACIFIC. For a brief summary of the temperature conditions of the North Pacific we may take a recent article by that eminent authority, Sir John Murray.* The charts which he gives afford * Murray, Sir John. On. the Temperature of the Floor of the Ocean, etc. Oeog. Jour. 1899, XIV, p. 34. 278 University of California Publications. [GEOLOGY a summary of a vast amount of observational detail bearing on the general problems of his paper. The charts showing maxi- mum and minimum surface temperatures will first be examined. These were prepared by laying off on 2 squares all the recorded observations of surface temperatures. The tables of Admiral Makaroff give 38,874 observations for the North Pacific. Murray has supplemented these by the reports of the British Admiralty Office and from other sources. The maximum and minimum temperatures are taken for the months of August and February respectively. Nearly 25% of the 2 squares in the North Pacific have no recorded observations. This lack should be borne in mind, but as nearly half of these omissions are in the Torrid Zone, it is not likely that the mapping of maximum or August temperatures in the broad belt of these charts has been seriously affected. Maximum Surface Temperatures. PL 34 B shows the results for the North Pacific, the temperature zones indicating difference of 10 F. So far as the problems of this paper are concerned, the most marked departure from east and west boundaries to these zones is found in the belt of 60-70. This shows a notable ex- tension southward along the coast of the United States and re- veals the belt of cold coast water, confirming the existence of a southward flowing drift off the coast, as shown on the Pilot Charts. The torrid belt of 80-90 makes a northward extension along the coast of Lower California. This again confirms the Pilot Chart which shows a northwestward flowing current off the Mexican coast. Minimum Surface Temperatures. PL 35 A is the chart for minimum surface temperatures in the North Pacific. Here again is the southward extension of the cold belt along the western coast of North America. An interesting fact here is the bend to the southward along the 120th meridian showing that the currents from the north leave the shores of America turning to the west- ward. Range of Surface Temperatures. PL 35 B is from another chart by Murray from the same data.* The annual range of tem- * Murray, Sir John. Annual Eange of Temperature, etc. Geog. Jour. 1898, Vol. XII, p. 113. BULL DEPT. GEOL. UNIV. CAL VOL. 4, PL. 35 A. Minimum Surface Temperatures, after Sir John Murray. B. Annual Kange of Surface Temperatures, after Sir John Murray. o a b GSO |.b *j a A VOL. 4] Holway.Cold Water Belt. 279 perature is here shown. The great torrid belt with an annual range of 10 or less shows a northward pointing extension off Lower California similar to that on the map of maximum temper- atures and to be accounted for in the same way. An interesting minor point, bearing on the accuracy of the map, is shown by the small area around the southern part of Lower California, which is charted as having an annual range of 20. This in- cludes the locality where Buchanan reports cold water due to upwelling. It will be seen by reference to the Pilot Charts that while the main current from the southeast is constant during the year, the inshore current varies with the seasons, sometimes being from the north and sometimes from the south. This varia- tion indicates of course a great annual range of temperature. This mutual confirmation of the two maps in this small area is worth noting as a correlation to the warning given by the authors as to the insufficient data upon which their work rests. Another variation in PI. 35 B is the southward extension of the belts of an annual range of from 10 to 15. This occurs at about 120 West Longitude and extends to Latitude 10. This is probably accounted for by a variation in the strength of the south flowing California current and of the northwest flowing current off Mexico. This variation is somewhat indefinitely shown on the Pilot Charts by a change in the extension of these currents during the spring and the autumn seasons. Temperature of Ocean Bottom. PI. 36 is a reproduction of the Deutsche Seewarte chart showing ocean depths in the North Pacific. The principal areas which according to Murray have a bottom temperature of under 35 are indicated by oblique pa- rallel lines. The contours on this chart are in meters; the first line indi- cating 200 m. and the others the successive even thousands. In the region to the eastward of Kamchatka these contours must be modified to agree with recent soundings of the Albatross. A sounding of 5,700 M. (3,117 Fm.) was obtained in Lat. 54-51', Long. 163-46' E and other soundings indicate that a channel of about 3,000 M. (1,640 Fm.) leads from the Pacific into Bering Sea. A dotted line shows the possible location of the 3,000 M. 280 University of California Publications. [GEOLOGY contour according to these late soundings. The distribution of these areas of cold water on the ocean bottom is closely related to the question of the- source of the cold water along the west coast of the United States. Of primary in- terest is the larger area extending from near Alaska south- ward far beyond Point Conception. The part of this mass of cold water lying north of Lat. 50 is bounded on the north and east by the contour line of 2,000 fathoms (nearly 4,000 M. ) . The western extension of this mass of cold and pre- sumably heavy water lies just on the edge or slope of a sub- marine valley that runs down to a depth of more than 3,000 fathoms (6,000 M.). If the distribution of cold water in the ocean depths depends on convection as is frequently claimed, why does not the cold water settle into this deep valley? This might be answered by supposing greater density for the water in the greater depths. A discussion of the varying salinity on the bottom of the ocean in this region is at present impossible from lack of accurate data. The uniform upper level of this mass of cold bottom water is an interesting point when the North Pacific Pilot Charts of this region are examined. In this great bight of the Alaskan coast there is represented an ocean eddy turning contraclockwise for three-fourths of the year and being reversed in direction during the winter months. Is it possible that this eddy maintains a mass of cold water at the bottom at a constant level? The idea of a casual relation here is so seduc- tive that the writer feels compelled, in fairness, to quote a para- graph from the Pilot Chart: "After a careful consideration of the reports of vessels cruising near the Aleutian Islands and in the Bering Sea, the Hydrographic Office warns mariners against placing too much reliance upon current predictions in that portion of the North Pacific." The warning is probably intended to apply to regions farther to the westward, but should be considered for this region as well. In connection with the question of the existence of this Alaska eddy, it is to be remarked that the isotherm of 55 bends to westward just south of Alaska in a way to confirm the existence of such an eddy. (See PI. 32.) Setting aside theories and keeping in mind the thought of the VOL. 4] Holway.Cold Water Belt. 281 level upper limit of the cold bottom water as mapped by Murray for the region south of Alaska, let us examine its great southward extension. From off Vancouver Island to San Francisco it has risen above the 2,000 Fm. (4,000 M.) contour and lies upon the conti- nental slope of the ocean bottom again in defiance of gravity unless there is postulated a peculiar arrangement of salinity in the lower depths. HYPOTHESIS ACCOUNTING FOR COLD WATER BELT. To explain this apparently abnormal position of the cold water, let us suppose, as a working hypothesis, that the direction of ocean drift in the northeastern parts of the North Pacific is not merely true for the surface, but that it holds throughout the entire extent as far as the ocean bottom. In winter the cold surface water to the south of the Aleutian Islands would sink and at the same time be carried slowly toward the eastward. It would thus be carried over the western portion of the Maury Deep of PI. 36 and would finally rest on the continental slope. In the Alaska Bight it is conceivable that the eddy would give a constant upper level to this mass of water. To the southward along the coast of Vancouver to San Francisco, the upper drift (except very close inshore) is toward the east and south. If this drift extends to the ocean bottom, the cold bottom water would be driven up the continental slope, thus accounting for the belt of cold coast water. Again it will be remembered that the coldest coast water was found from the vicinity of Cape Blanco southward to Cape Mendocino. In PL 36 the contours of 1,000, 2,000, and 3,000 meters make a shoreward bend slightly north of this latitude. That is, a great submarine valley heads just under Cape Blanco and opens broadly out to the northward and westward. The bottom drift on our working hypothesis would thus be delivered most strongly against the coast in the vicinity of Cape Blanco and carried southward by the general drift, 282 University of California Publications. [GKOLOGY The effect of the smaller submarine valleys near the coast has already been discussed by Davidson.* Speaking of those near Cape Mendocino he says: "They carry in the colder waters coming from the north and outside of the influence of the close inshore eddy current setting to the northward. ' ' The writer fully agrees with this statement, but in the light of the additional data discussed in this paper, he considers the action of these valleys as but part of a general motion of the deeper waters which affects the entire coast from San Francisco to Vancouver Island. Another instance where local temperatures seem to be influ- enced by submarine valleys is found on Cordell Bank about 50 miles w r est-northwest from San Francisco and directly west of Point Reyes. The 100 Fm. contour shows a valley opening to the northward and heading just east of the Cordell Bank. From June 12 to 17, 1873, Davidsonf reports the mean water temperature at 8 a.m. as only 49. If the cold bottom water in the deeper ocean has any motion or drift, it is not difficult to recognize the fact that the submarine valley to the northward might lead it to the surface in the vicinity of Cordell Bank. A second point in favor of the theory of great depth to the prevailing drift in the northeastern part of the North Pacific is found in the shape of the areas of cold bottom water and in their relation to the surface drift. The main area on the west coast of North America has a longitudinal extension that agrees with the prevailing surface drift. Tracing this area of cold bottom water southward to Lat. 30, it is seen to bend to the southwestward as do the surface currents. The question also arises as to the reason for a termination of the cold water at this locality. It is certainly not the insolation received in the torrid zone, for this penetrates but a short distance below the surface of the ocean. Moreover, in the middle of the North Pacific ex- tending across the equator into the southern hemisphere is one of the largest areas of water below 35 on the ocean bottom. A ready explanation for the termination of the cold bottom water * Davidson, Geo. The Submerged Valleys of the Coast of California, etc. Pro. Calif. Acad. Sci., Geol. Vol. I, p. 99. t Davidson, Geo. 'Pacific Coast Pilot, p. 236. VOL - 4 ] Holway.Cold Water Belt. 283 off Lower California is found in the northwest flowing warm Mexican current previously mentioned. This current, accord- ing to the charts of the Deutsche Seewarte, is more saline and hence will sink and mingle with the colder water from the north- ward. Another interesting area of cold water on the ocean bottom is found off Japan in the great Tuscarora Deep. The source of this cold water is doubtless the cold polar current coming down by Kamchatka. The southern part of this cold water area has an extension off to the eastward. It has a direction that appears to be the resultant of a conflict between the deep part of the north-flowing Japan stream and the cold water of the Kamchatka current. Here again the idea of great depth of drift would account for the fact that we have represented a stationary body of cold water resting on the sloping ocean bottom. Of course, the hypothesis that these ocean currents and drifts have a uniform direction to the bottom of the sea needs additional evidence in its support. Meanwhile it offers a reason- able explanation of the cold coast water on the North American shore and of several peculiarities of the masses of very cold water on the bottom of the North Pacific with little indirect op- position to the hypothesis. The presence of the large area of cold water on the bottom of the south central portion of the North Pacific here challenges attention. Can it be accounted for by the known direction of surface or bottom drift? It must have some connection with the cold water of high latitudes to maintain its low temperature of 35 or under. There is no evidence to connect it with the cold water off North America. From its position in equatorial regions it must necessarily be supplied by subsurface currents. There are few charts showing temperature below the surface in the North Pacific. Turning to one by Makaroff* for the level 400 meters (218 Fm.) below the surface, the isotherms are found to make a sharp bend to the southeast as may be seen in PL 37. This indicates a southeast flowing portion of the cold Kamchatka current which has underrun the warm Japan stream. The * Makaroff, S. Le Vitiaz et L 'Ocean Pacifique. 284 University of California Publications. [GEOLOG\ writer attempted to construct an isothermal chart for the depth of 700 Fin. in order to follow further this cold undercurrent. The number of temperature observations for this or greater depths is few, and therefore not much reliance can be placed in the results. The isotherms as drawn for the 700 Fm. level show a narrow loop extending still farther to the southeast than the loop in PI. 37. It would thus seem from the evidence now at hand that the cold water at the bottom of the south central portion of the North Pacific is accounted for by a branch of the Kamchatka current underrunning the upper portion of the warm Japan stream and slowly sinking to the bed of the ocean. In the provisional isothermal chart drawn for the depth of 700 Fm. a second narrow loop of the isotherms, starting farther to the east of the Japan Islands, runs southeast toward the Hawaiian Islands. This would account for the presence of water below 35 F. that occurs to the northward of these islands at the depth of 2,500 Fm. The study of the areas of cold water at the bottom of the central portion of the North Pacific does not therefore in any way contradict the hypothesis used for the cold water belt along the west coast of the United States. In the northwest due to the opening into Bering Sea between Kamchatka and the Aleu- tian Islands, a southward flowing cold current disturbs the otherwise great uniform clockwise drift of the North Pacific. In the north central and northeastern portions of the ocean there are no cold currents from Bering Sea to interrupt the ac- quirement of a uniform direction of drift to great depths. The possibility of water at a great depth acquiring a slow movement or drift from the action of surface winds has been frequently discussed. A recent writer* thinks that the entire body of water occupying the equatorial regions has a westerly motion due to the action of the trade winds. In the northern parts of the Pacific in the region of the prevailing westerlies, contrary currents are frequently reported more or less in har- mony with variations in the winds. But as the prevailing westerlies have existed for untold ages, there has been ample * Page, James. National Geographic Magazine, 1902, pp. 135-142. e! Jj o VOL. 4] Holway.Cold Water Belt. 285 time for the development of a slow but constant deep water movement in the direction of the prevailing wind. The north- eastern part of the North Pacific is pre-eminently the place for the development of a uniform drift from surface to bottom, as may be seen by studying the contours in PL 36. The contours show a remarkable great ocean basin uninterrupted by islands and bounded on the north and east by a regular but steep con- tinental slope. This regularity of basin of the North Pacific is more noticeable if for comparison we examine a bathymetrical chart of the North Atlantic. In the latter we have the mid- Atlantic ridge running in a general north and south direction and making two great subdivisions of the basin. We have also the wide openings on the west and on the east of Greenland and connecting with the cold water of the Arctic Ocean. In the Pacific there is but one great opening into Bering Sea and that sea is connected with the Arctic by Bering Strait, which is both narrow and shallow. Considering then its practical lack of connection with the Arctic Ocean and its uninterrupted basin and relatively regular shores, it is a reasonable supposition that the northern half of the North Pacific has a more regular system of oceanic circulation than has the North Atlantic. SUMMARY. Several interesting points for future investigation are sug- gested by the observations and theories discussed in this paper. From the biological standpoint it will be interesting to find whether the cold water and the variations in temperature near Cape Blanco are a barrier to species that might normally ex- pand into the regions lying to the northward. The investiga- tion of the area lying to the southwest of the coast from Point Conception to San Diego, now being carried on under the direc- tion of Professor William E. Hitter of the University of Cali- fornia, should in the next few years give us more accurate in- formation concerning the disputed temperature relations of this portion of the Pacific as well as a better knowledge of the marine life of the region and the temperature limitations of this life. 286 University of California Publications. [GEOLOGY The question of the accuracy of the charts herewith pre- sented demands that the various gaps in the series of coast tem- peratures be filled by reliable observations. If the theory of this paper as to the final source of cold water lying along the west coast be correct, serial temperatures in the region from 50 to 55 N. Lat. and about 160 W. Long, should show, at certain seasons of the year, inversions of temperature, that is, a stratum of cold water should be found in intermediate depths overlying warmer water on the ocean bottom. In conclusion the following summary of observations and hypotheses in reference to the belt of relatively cold water lying along the west coast of the United States is presented : (1) Recent observations indicate that the previous mapping of this cold belt as extending southward to the coast of Lower California is incorrect. The definite belt of cold water can not be traced south of Point Conception. (2) In summer the coldest part of this belt is in the vicinity of Cape Blanco and Cape Mendocino. (3) The source of this cold coast water is in the ocean depths to the northwestward. (4) This cold water at or near the ocean bottom has a slow drift agreeing in direction with the average direction of the surface drift and is driven to the surface on striking the slope of the continental shelf. Local variations in the cold coast water are due to the submarine valleys and other irregularities in the slope of the continental shelf. University of California, September, 190~>. VOLUME 4. PRICE 1. The Geology of the Upper Region of the Main Walker River, Nevada, by Dwight T. Smith 30c 2. A Primitive Ichthyosaurian Limb from the Middle Triassic of Nevada, by John C. Merriam lOe 3. Geological Section of the Coast Ranges North of the Bay of San Francisco, by V. C. Osmont 40c 4. Areas of the California Neocene, by Vance C. Osmont ....... 15c 5. Contribution to the Palaeontology of the Martinez Group, by Charles E. Weaver . . 20c 6. New or Imperfectly Known Rodents and Ungulates from the John Day Series, by William J. Sinclair .............. 7. New Mammalia from the Quaternary Caves of California, by William J. Sinclair 8. Preptoceras, a New Ungulate from the Samwel Cave, California, by Eustace L. Furlong lOc 9. A New Sabre-tooth from California, by John C. Merriam ...... 5c 10. The Structure and Genesis of the Comstock Lode, by John A. Reid ..... loc 11. The Differential Thermal Conductivities of Certain Schists, by Paul Thelen . . . 25c 12. Sketch of the Geology of Mineral King, California, by A. Knopf and P. Thelen . . . 35c i:i. Cold \Yater HHt Along the West Coast of the Tinted States, by Ruli If S. flolway . 2i><- LIBRARY USE HBN TO DESK i-,r ,. MAIN UB *ARY "!S?5^ N DEp ARTMENT -. (B227S10)9412-A32 .General Library University of Calif ornia Berkeley NON-CIRCULATING BOOK UNIVERf 5m-9,'26