' ‘ 1 +4 ‘ ' H ‘ { i: }o4 Hi y 74S .48 tis Pac | ,a4 a aon Aga u qq | oe Be Pak OP 13.4 ; t4 ‘ 14 AT TOM A Me ee a a "4 t L2ti 4g . 58 Fae ‘ 44 ‘ i : «= ha i t 44 i444 oe ‘ v.n 3 4 L) tv! . 1 ‘ { ie | | t thy Pe he ee! : : ‘ ‘ rays 4 13 \ oe ‘ ‘ ‘ ‘ | a , ’ ' } ee ne rome: i : si a He tees teen pmaoees + Hee i! sions fy Hf if it i) i Wir Henn if a4 aH KK Hae erie i i ARH Meet aa ‘ Y ah ft) Ne ( ee ee) sty } tye ONaN a Se 8 i SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 > “EVERY MAN IS A VALUABLE MEMBER OF SOCIETY WHO, BY HIS OBSERVATIONS, RESEARCHES, AND EXPERIMENTS, PROCURES KNOWLEDGE FOR MEN’’—JAMES SMITHSON (PusticaTion 4311) CITY OF WASHINGTON PUBLISHED BY THE SMITHSONIAN INSTITUTION 1958 LAW OAH Tite P AMOITIAIIOD ZIOTSA Lim ; MU sHisti '! Sar ¥YEo morse UATHOMEING ST Ve qeveigadyyy a na \ F bri ; ie le 0) ; i 7 i otek ry) , ADVERTISEMENT The Smithsonian Miscellaneous Collections series contains, since the suspension in 1916 of the Smithsonian Contributions to Knowledge, all the publications issued directly by the Institution except the An- nual Report and occasional publications of a special nature. As the name of the series implies, its scope is not limited, and the volumes thus far issued relate to nearly every branch of science. Papers in the fields of biology, geology, anthropology, and astrophysics have predominated. LEONARD CARMICHAEL, Secretary, Smithsonian Institution. (iii) 10. iT. 12. CONTENTS Assot, C. G. Periods related to 273 months or 22} years. 17 pp., 7 figs. Sept. 13, 1956. (Publ. 4265.) DeicNAan, H. G. The Asiatic species of birds of the genus Criniger (Pycnonotidae). 9 pp. Oct. 25, 1956. (Publ. 4266.) Cooper, G. ArTHUR. Loop development of the Pennsylvanian terebratulid Cryptacanthia. 18 pp., 2 pls., 12 figs. Jan. 31, 1957. (Publ. 4267.) TourtELot, Harry A. The geology and vertebrate paleontology of upper Eocene strata in the northeastern part of the Wind River Basin, Wyoming. Part 1. Geology. 27 pp., 1 pl., 7 figs. Mar. 27, 1957. (Publ. 4269.) SAUNDERS, JoHN B. Trochamminidae and certain Lituolidae (Foraminifera) from the Recent brackish-water sediments of Trinidad, British West Indies. 16 pp., 4 pls. Mar. 15, 1957. (Publ. 4270.) GREGOIRE, CHARLES. Studies by phase-contrast microscopy on distribution of patterns of hemolymph coagulation in insects. 35 pp., I pl., 4 figs. May 8, 1957. (Publ. 4271.) Ewers, Joun C. Early white influence upon Plains Indian painting. George Catlin and Carl Bodmer among the Mandan, 1832-34. I1 pp., 12 pls. Apr. 24, 1957. (Publ. 4292.) Gazin, C. Lewis. A skull of the Bridger middle Eocene creo- dont, Patriofelis ulta Leidy. 20 pp., 4 pls. Apr. 30, 1957. (Publ. 4293.) Wetmore, ALEXANDER. The birds of Isla Coiba, Panama. 105 pp., 4 pls., 15 figs. July 8, 1957. (Publ. 4295.) Roru, Lours M., and Wittis, Epwin R. The medical and vet- erinary importance of cockroaches. 147 pp., 7 pls. Dec. 19, 1957. (Publ. 4299.) “Levine, Harvey R. Anatomy and taxonomy of the mature naiads of the dragonfly genus Plathemis (family Libellulidae). 28 pp., 25 figs. Sept. 25, 1957. (Publ. 4301.) Coorer, G. ArTHUR. Permian brachiopods from central Oregon. 79 pp., 12 pls., 2 figs. Dec. 9, 1957. (Publ. 4302.) (v) SMITHSONIAN MISCELLANEOUS COLLECTIONS VOLUME 134, NUMBER 1 Roebling Fund PERIODS RELATED TO 273 MONTHS OR 22-3/4 YEARS By ' C. G. ABBOT Research Associate, Smithsonian Institution H eneee Pre (PuBLicaTION 4265) CITY OF WASHINGTON PUBLISHED BY THE SMITHSONIAN INSTITUTION SEPTEMBER 13, 1956 THE LORD BALTIMORE PRESS, INC. BALTIMORE, MD., U.S.A. Roebling Fund PERIODS RELATED TO 273 MONTHS OR 22% YEARS By C. G. ABBOT Research Associate, Smithsonian Institution This period was discovered in the variation of the measures of the solar constant of radiation, made daily by the Smithsonian Astro- physical Observatory from 1920 to 1952. It was first glimpsed in 1935,' and noted in various terrestrial phenomena, such as tempera- tures, precipitation, width of tree rings, and levels of lakes. The level of Lake Huron, since 1837, has followed related periods of about 23, 46, and g1 years. I ventured, in 1938, to predict droughts during the 1950’s, the 1970's, and the 2020’s, based on recurring periodic de- pressions of the level of Lake Huron. The first of these predictions is now verified. 1, PERIODS FOUND IN SOLAR-CONSTANT MEASUREMENTS The “solar constant of radiation” is the term in use to describe quantitatively the intensity of the sun’s radiation, as it would reach points in space outside the earth’s atmosphere, at the earth’s mean distance from the sun. Smithsonian measurements over many years, made at stations rang- ing from sea level to 14,400 feet altitude, and supplemented by auto- matic records at 15 miles of elevation from sounding balloons, yield as the value of the solar constant 1.946 calories per square centimeter per minute. A recent revision by F. S. Johnson,? in which he used the latest data from high rocket flights to improve the Smithsonian estimates in the extreme ultraviolet spectrum, yielded the value 2.00 cal.+0.04 cal. His value differs from the Smithsonian value by little beyond the probable error of either one. For purposes of estimating solar periodic variations, this small difference as to the basic value is inconsequential. 1C. G. Abbot, Solar radiation and weather studies, Smithsonian Misc. Coll., vol. 94, No. 10, 1935. 2 Journ. Meteorol., vol. 11, No. 6, December 1954. SMITHSONIAN MISCELLANEOUS COLLECTIONS, VOL. 134, NO. 1 2 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 What is important for the proof of variation is the accidental error of Smithsonian daily observations of the solar constant. There are several determinations of it. From volume 6 of the Annals of the Smithsonian Observatory, page 163, I quote the differences, in thou- sandths of a calorie, between daily values of the solar constant ob- tained at Smithsonian stations in the Northern and the Southern Hemispheres, respectively. This comparison covered all days observed in both hemispheres for the years 1932 to 1936, numbering 616. Taste 1.—Numbers of daily differences in solar-constant measures, 1932 to 1936, having different amplitudes. Amplitudes in thousandths of a calorie. Amplitudes .... 22-28 20-22 18-20 16-18 15 14 12 vi 10 No. of days.... 17 12 10 35 13 15 20 22 2 PEOGUCE os oneness 201 .262. 100 505. 105 210 240 242..270 Amplitudes .... 9 8 Gi 6 5 4 3 2 I te) Ne Of idays oo. 3d 30. S85 AB BE 55. 550,437 nity Sena Prodgct a. a 300 240 -245 (258.5255 .220 , 105 74 48 fe) Total days 616. Total of products 4,682. Weighted mean daily difference, 7.60 thousandths of a calorie. Mrs. Hill has made for me similar tables for more recent differences between daily solar-constant results, where measures at Montezuma, Chile, are compared to those of Table Mountain and Tyrone in the United States, and those at Table Mountain, Calif., to those at Tyrone, N. Mex. For these three cases the weighted mean differences are 7.68, 7.96, and 7.79 thousandths of a calorie. These results cover all days measured at both stations from 1940 to 1952. They number, respec- tively, 891, 283, and 202 days. The weighted mean difference is 7.75 thousandths calorie. As the results of these recent years differ but slightly from those of 1932 to 1936 shown in table 1, we may adopt 7.7 thousandths of a calorie as the weighted mean average daily acci- dental difference between results of widely separated stations observ- ing the solar constant. Assuming the stations to be of equal accuracy, that gives for the percentage accidental error of a solar-constant measure of one day at one station: 100 X 0.00385 Xx 0.84 + 1.946=0.166, or % percent of the solar constant. I use 10-day and monthly solar-constant values in my investigations. For these the percentage probable error (if all days of these intervals were observed) becomes %+ V10 and %+ 30, or Mo and %s per- cent of the solar constant. NO. I PERIODS RELATED TO 273 MONTHS—ABBOT 3 A single supposed periodic appearance from mean monthly data, with an amplitude four times as great, or %3 percent, would have some claim to veridity. Using monthly means from 1924 to 1952, 348 in number, all periods shorter than 45 months would have 8 or more repetitions. The criterion for probable veridity would be a percentage range exceeding 43+ WV8=%s percent of the solar constant for a 45-month period. The requirement decreases as the square root of the number of repetitions increases. Thus for a period of 4% months, my shortest used in syntheses, it would be %2 percent. The %3 percent of the solar constant is 0.0008 calories. RANGES OF PERIODS IN SOLAR-CONSTANT MEASURES, WHICH ARE ALIQUOT PARTS OF 273 MONTHS In my paper “Periodic Solar Variation,’ * I list in table 2 64 periods. They range in amplitude as follows: TABLE 2.—Ranges of periods discovered, in percentage of the solar constant ietiods ATITEIONEMS s xs) o:sfae ies 136.5-45 30-25 23-15 14-10 10-6 5-4.5 BUEN Sele facicte,cuscé c #5, 0-c0.0 « 5 5 5 5 5 5 Wmplitudes, % ............ 0.09-0.18 0.05-0.2I 0.03-0.08 0.02-0.I1I 0.06-0.13 0.02-0.08 Periods in months.......... 4.4-3.7 3.5-2.9 2.7-2.4 2.1-1.7 1.7-1.3 0.02 All these 64 periods, so far as ranges of amplitude indicate, fall within the criterion for veridity based on accidental error of observa- tion. OTHER EVIDENCES OF VERIDITY Referring again to the last-cited paper, figures 1 and 2 therein show how the curves of observed periods which are aliquot parts of 273 months stand out more and more plainly, as superriding periods whose lengths are also aliquot parts of 273 months are removed. Figure 3 of that paper shows how strongly the smoothed curves resemble sine : curves when cleared of such superriders. Still more convincing indications of the veridity of a large number of the periods found in solar-constant measures will appear in follow- ing sections, as we note how periods in quite different phenomena are identical with them. 8 Smithsonian Misc. Coll., vol. 128, No. 4, 1955. 4 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 2. PERIODS RELATED TO 273 MONTHS FOUND IN WEATHER In an important paper published in 1947,* I discovered, both in solar variation and in Washington temperature departure from normal, a period of 6.6456 days. This solar periodic variation recurred with perfect regularity in its phases from 1923 to 1944. The Washington periodic variation in temperature departures, though frequently out of phase, yet for any single month of the 12 months of the year in the entire interval from 1910 to 1945 averaged exactly the same length as the sun’s variation, namely 6.6456 days. I did not then understand why phase changes occurred from time to time in Washington tem- perature departure. It is now quite clear to me, as will appear below. Not until 1953 did I perceive that this period of 6.6456 days, so strongly evidenced, belongs to the family of submultiples of 22% years. For 22% xX 365.2564 days=8309.5831 days. Dividing by 6.6456, we have 1250.38, or within %o percent of 1250. So it is prob- ably an exact submultiple of 273 months, to an accuracy far beyond the precision of the data. In the years 1952 to 1955 I published eight papers on the control of weather by the family of periods related to 273 months.® Before particularizing these weather investigations, I wish to emphasize that they stand entirely on meteorological records. Meteor- ologists are apt to say that the variations of the sun are too small to influence terrestrial weather appreciably. But solar-variation measures play no part in my studies just cited. The periodicities in weather which relate to 273 months are to be found in weather records them- selves. No further reference to solar measures is required. Periodic variations in precipitation are large. They range from 5 to 25 percent of normal for the individual periodicities. In temperature departures they range up to 5° F. These large periodic changes of weather related to 273 months lie buried in the published records and may be demonstrated from them. No reference to solar variation is required to find them. 4 The sun’s regular variation and its large effect on terrestrial temperatures, Smithsonian Misc. Coll., vol. 107, No. 4, 1947. 5 Periodicities in the solar-constant measures, Smithsonian Misc. Coll., vol. 117, No. 10, 1952; Important interferences with normals in weather records, associated with sunspot frequency, ibid., No. 11, 1952; Solar variation and precipitation at Peoria, Illinois, ibid., No. 16, 1952; Solar variation and precipitation at Albany, N. Y., ibid., vol. 121, No. 5, 1953; Long-range effects of the sun’s variation on the temperature of Washington, D. C., ibid., vol. 122, No. 1, 1953; Solar varia- tion, a leading weather element, ibid., No. 4, 1953; Sixty-year weather forecasts, ibid., vol. 128, No. 3, 1955; Periodic solar variation, ibid., No. 4, 1955. No. I PERIODS RELATED TO 273 MONTHS—ABBOT 5 These periodicities in weather cannot be satisfactorily demonstrated without attending to several steps made necessary by changes of the atmosphere. 1. Normals and departures must be separately tabulated for times of high Wolf sunspot numbers, and of low Wolf numbers. I am accustomed to drawing the line at 20 Wolf numbers. 2. For all the shorter periods (1.e.,.<15 months) the months of the year must be used in several separate groups because atmospheric conditions differ. I am accustomed to dividing the year into three groups: January-April, May-August, September-December. I omit this grouping after periods of 15 months. Beyond that, too few col- umns would generally be available in a tabulation, and the division of the year into several groups is less important compared to the length of periods. The division of data into three groups mentioned above indeed leaves the tables with too few columns to yield satisfactory means. Therefore I make the assumption that the form and amplitude of periods in different seasons will be sufficiently similar to permit combination of six separate tables for the three seasons and two ranges of Wolf numbers into one by shifting them all to a common phase. But when such a combined table is used in a synthesis its gen- eral mean must always be restored to the proper phase in the synthesis. 3. As the earth is copiously bombarded with solar ions when sun- spots are numerous, and these ions act to produce haze in the at- mosphere, it is also necessary to separate tabulations for high and low Wolf numbers. I am accustomed to drawing the line at 20 Wolf numbers. 4. As the growth and shifting of populations and the invention of new devices, such as automobiles and airplanes, operate to alter the atmosphere, it is necessary to make a division of data for this. I am accustomed to drawing the line at the year 1900. That is not really adequate, but perfection is beyond reach, for with 23 periods to be synthesized, the precautionary measures mentioned above require 186 tables to be used. 5. As there are many periods, all exact aliquot parts of 273 months, it follows that most tabulations for a selected period are encumbered by shorter periods, exact aliquot parts of the period tabulated. I am accustomed to plotting the mean result of such a tabulation, scanning the graph for superriders, and, one after another, computing form and amplitude of these superriding periods, and removing them by sub- traction till the wanted period stands out alone. 6 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 SOME RESULTS OF STUDIES OF WEATHER PERIODS “Sixty-year Weather Forecasts,” my Saint Louis precipitation paper, may be thought to have a sensational title. Critics are apt to say that when I use all the monthly mean values of precipitation at Saint Louis from 1854 to 1939 as a basis to determine the form and amplitude of 23 periods, no part of the synthesis of them between these dates is a forecast. On the contrary, 1,032 months are used to determine the features of these periods. No year has more than 12 months. Hence the form and amplitude of the curve representing the march of precipitation in any one year between 1854 and 1939 can 12 have no more than 10 =1I.2 percent influence on that year’s curve. 2 Therefore, each year’s march of precipitation between 1854 and 1939 is practically an independent forecast. After 1939, up to 1957 when my synthesis ends, all years are completely independent forecasts. As the halfway point between 1854 and 1939 is the year 1897, forecasts may be regarded as made from 1897. Thus, speaking approximately, every year from 1854 to 1957 is forecasted as if from 1897. As a fair specimen of such forecasts, I cite from “Sixty-year Weather Forecasts’: figure 1 (here fig. 1), a facsimile of the 5-year Saint Louis forecast, 1875-1879; figures 2, 3, and 4 (here fig. 2), comparing forecasts with events for 6-year intervals, 1934-1939 in percentages of normal in the precipitation at Peoria and Saint Louis, and in the temperature departures from the normal at Washington, D. C.; and figure 5 (here fig. 3), comparing synthesis and event for Saint Louis precipitation, 1800-1887. Finally, I cite figure 6 (here fig. 4), comparing predictions for 1952-1957 of precipitation at Saint Louis and Peoria, prepared, of course, from wholly independent data. The predictions are in effect based on the year 1897, the halfway point between 1854 and 1939, which were the extremities of the basic interval employed. These two stations, Saint Louis and Peoria, are about 100 miles apart. Their 60-year forecasts run almost parallel. Both indicate the approach in 1952, waxing, maxi- mum severity in 1956, and probable end of the drought in 1957. The tabulation of Saint Louis precipitation for 104 years (1,248 months) is preserved at my home in a roll 25 columns wide, 1,248 lines long, and about 20 feet from end to end. Comparing its two curves of synthesis and event for 100 years, 1854-1954, 70 of the 100 years were of the same degree of similarity in time, form, and amplitude of range, shown by figure 3 of the present paper. In the other 30 years the features of the parallel curves were similar, but NO. 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Data from monthly mean precipitation smoothed by 5-month running means. Dotted curve from summation of 22 regular periodicities, determined as averages over the 84-year epoch, 1854-1939. Full curve, the event. displaced one or more months. These displacements seemed generally to follow either great volcanic eruptions, such as Krakatoa, Colima, and Katmai, or great bombing periods, as in the war years 1916-1918 and 1940-1945, and recent tests of atomic bombs. The results, though subject to such blemishes, seem to offer a useful means of mapping countries for decades in advance to exhibit probable precipitation in percentages of the normal. Suppose 50 VOL. 134 SMITHSONIAN MISCELLANEOUS COLLECTIONS "juaad ay} ‘Aino [Ny { payndwios ‘aasnd payjog “yuaaa ay} 0} pasedwoo uorjeydisaid sinoT “3S JO ‘Zggi-OggI ‘suotyeyduod jo sIsayJUAG—E “Oly ee ae %* TE rales Ls een ae Senos Set "sues SuluUNI poyjJoous YyUOUI-S WOT} [[Y ‘S}UoA9 ‘s9Aand ][N} {payndusod ‘sadamd pa}oq ‘Teullou wos sainjredap ‘einjzesodurs} ‘[euI0U Jo sasequesiad ‘uojepdioasg “s}uaAa ay} 0} Paseduio0d 6£61 -P€61 suorjeynduiod (stno7T 3G) sinyeIedwi9} pue (soy 3S pue eliosg) UOHeydIaIg “eoueApe UI sivah oF suonsipeid seah-9 V014 [—Z “SIT SSRI ee ai CO TRE RATT Bs <> ett | i=. aid i os ne eaeaie et Mb od BE i AIOE OIE Pe eet ' (ae ae STHLNAS FIHINIG| ===> wij INIA [—— Veda | |sinoy ag NOrLPLIdI DIY! SIMO AS SIMLNAS tNAJ atataNg uF are = No. I PERIODS RELATED TO 273 MONTHS—ABBOT 9 stations east of the Rocky Mountains in the United States were treated as I have done at Saint Louis, Peoria, and Albany. Lines of equal probable percentage of normal precipitation could be drawn for each season of the year for Io years in advance. A success of 70 percent, as in Saint Louis, would be a boon to industry, and moderate phase displacements in 30 percent would be no serious failure. After all, it is seasonal weather that is most desired to be known. Three-month averages would remove most of the blemishes. EE IMANAIN ee, Pe YY is AIENEaEESUES JARI AVAL GTT A BaA | CCN ak —— Fic. 4.—Predicted precipitation, Peoria (upper) and St. Louis (lower), 1952- 1957, from mean forms of 22 periodicities over the epoch 1854-1939. End of prediction 18 years after 1939 and 60 years after middle of base, 1897. Dotted curves, prediction; full curves, event. Horizontal lines represent normal pre- cipitation. Drought indicated ending 1957. 3. SNOW-COVERED DATES AT TOKYO, JAPAN My friend Dr. H. Arakawa recently published * dates of the earli- est wintry snow coverage for Tokyo since 1632. Many years are missing, but about 200 years are included. Dr. Arakawa treats the data very interestingly, but in Iarge groupings. It occurred to me to plot all the dates of first coverage, reckoned after November 30, in days for each year given. I plotted blank years in the same regular order as the rest. Though the long plot showed many breaks, I seemed to see in it a tendency to a period of 45% years, twice 273 months. 6 Quart. Journ. Roy. Meteorol. Soc., vol. 82, No. 352, p. 222, April 1956. Io SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 I then tabulated all the data. The mean march of them is shown in curve A, figure 5. A period of 45%4+3, equaling 15% years, seemed indicated, as shown in curve B. Subtracting its smoother ordinates (42+smoothA ), the final column of the mean table, A, results, and is plotted in curve C. Though rough, a period of 45% years, with an amplitude of 8 days, is found. The smoothed curve B for 15% years has the amplitude of 7 days. From curve C, one would expect a snow coverage at Tokyo averaging a week earlier for the years 1955-1970 than the average which prevailed from 1930-1945. Casting the eye along any of the 45 lines of the table (fig. 5), one sees no well-marked tendency for a change in amplitude at any phase of the 45'4-year period from the seventeenth to the twentieth century. GLACIAL ADVANCES RELATED TO 273 MONTHS I recently received from the author, Herbert Griinhagen of Stadt- oldendorf, Germany, a paper entitled “Die Klimawellen der Fiszeit.” * He refers to a beautifully printed small book by W. Soergel, professor of geology and paleontology at the University of Freiburg, entitled “Die Vereisungskurve.” ® In this paper Soergel gives a curve to represent the fluctuation of latitudes of ice penetration in central Europe as glaciation advanced and receded from the direction of Sweden. Griinhagen smooths Soergel’s curve by using mean values for each successive 65,000 years. The curve thus treated he plots in 102 points, covering the interval from minus 565,000 to minus 30 years earlier than the year 1800 of our era. Griinhagen’s prior researches had disclosed to him periodic varia- tions related to various phenomena. He had noted that when such a period was found, the double of it was also apt to be a recognizable period in the phenomena. In these circumstances, a copy of my paper “Sixty-year Weather Forecasts” came to him, and some of the solar periods I used agreed closely with some periods he had found. He calls attention to families among my solar periods, in one of which the periods go in the order 1, %, %, %; and another in which the order 1, %, %, 442 is found. It occurred to Griinhagen to see if longer periods than mine, in- creasing by powers of 2, might perhaps be found in the smoothed Soergel curve. He puts forward six such periods as follows: 15 years multiplying by 2", 2'*, 2%*, yielding 61,440, 122,880, and 245,760 7 Separate from Niedersachsen, a periodical for home and culture, Heft 1, 1956. 8 Published by Borntraeger Brothers, Berlin, 1937. Il PERIODS RELATED TO 273 MONTHS—ABBOT I NO. wu 36 ) » Si yg L 2 Bh = fale bord todoa. Pepe avtere & 3 se by as TOY ay Be ous putt ioce ee = - ‘ & ~~ Yr a SO J Soh= Merry ak Naini 'ait haa eetess sete, H 20 é D | oo ese mM Metres Se se) LLQNTROLOS POTTEs TOP T POG aes q O—aM ¥ ADO~ io O=AUNT HYVER OH O—U OPH O~—aoWN an Orc Eff Fooneag MY) Seg= NOE wor ang-worseNwag=woemER WeRReseeSIRSSHE s © we Ly Sa Ye! soe ISAS rt tor PGMRVISe eee Cc AR CHEST SLIGHT E TH TLE GAL SIGHS F 2kn —W on =o w& =NMTNVE DHS ~—cuMmTtNVpn o- =~ ° nla HY RRB HToO ong) UOT ONDOS 2 . WNO~ VN 9 STayResesssenes a Sti LTD PEM or eo W TERIA TRVPRT Hg =! Ps. < o~- HON O~—aAMYP HY SL AIWTAVN OH Now fpor wag NMTH OM NAS NOY Nd a) Fic. 5—Snow coverage of Tokyo (Arakawa). The periods of 15% and 45% years are multiples of 273 months. Periods in years I2 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 years; also 11.25 years multiplied by 2%, 21°, 2° yielding 184,320, 368,640, and 737,280 years. Griinhagen publishes, along with Soergel’s smoothed curve of lati- tudes of penetration, another curve made up, as he states, from these six periods. The parallelism is striking. I could not interpret from Griinhagen’s paper how he obtained the phases, forms, and amplitudes in which he combined the six periods which he formed out of my 273-month solar period. I therefore read off 102 points of his smoothed Soergel curve. I computed from them the mean forms, phases, and amplitudes of the four shortest of Griinhagen’s six periods. The longer two were not repeated enough times to compute good mean values. However, as I have found all my solar periods to be exact submultiples of 22% years, I used for these four Griinhagen periods 74x (2"%, 24, 215) and 22%~x (23%, 2'#, 215). This gives for my first three periods the same values as his first three, but for my last three 186.4, 372.7, and 745.5 in thousands of years, instead of the value which he based on 11.25 years. In the following table I give the mean latitudes computed from the smoothed Soergel curve to suit periods of 61.4, 122.9, 186.4, and TABLE 3.—Glacial periods synthesized 61,400 122,900 186,400 245,800 Soergel smoot | Mean A Mean A ean A Mean 2A+56°8 curve 0.7DA+56°8 S750)! Ore 55:9 —o°8 55°3 —1°3 68:7. 187 —022 56°6 59°4 —Oo° 56.8 0.0 56.0 —o.7 55-4 —I1.2 59:0)" 2.0 0.1 56.9 59.3 oO. Ba Ti (Ong 56.2 —O.5 55.6 —1.0 5023). 2.3 A.I 57.9 59-4 O°. 57.0. 10,2 56.2 —0.3 56.0 —o.6 60707, “3.0 2.3 Sg. 60.5 I. E70" iOn2 56.6 —o.I 56.4 —0.2 60.6 3.6 30/5 60.3 61.2 as 56.8 0.0 56.7 0.0 Boaz | 0.5 Hows. 4.5 3.6 60.4 61.4 ae 56.7 —o.1 56.7. 0.0 S71 0.5 6025.7) 35 3-9 60.7 61.3 ae 56.7 —o.! B7.0 0.3 57-4 0.8 60.5 3-5 4-5 61.3 61.3 a 56.7 —o.1 57.0; (0'<9 Rea Lod. (ep ase NS 6.3 63.1 61.8 4 56.7 —o.1 57-9 mee 58.3 ad 61.5 4-5 7.3 64.1 62.1 a 56.6 —o.2 Soca, SAS 58.4 1.8 62.1 Bre x 8.2 65.0 62.5 ae EG. 8: i070 58.2 1.5 EOL =~ 20 62.7. 5.7 9.2 66.0 63.0 6. top 0.2 58.2 Te7 59.0 2.4 62.7 ° 5.7 10.0 66.8 63.6 Wis 0.0 50.04 ekr.4 So.g ) 2a7 6250) 5.0 9.1 65.9 63.3 6 0.3 58.1 0.8 59.4.% 269 Grit aun 8.0 64.8 62.7 Bie 0.2 57.5 1.0 59.1 2.5 60.7 Brat 7-4 64.2 61.6 5. ‘Orn 57.4 © 0.7 Bee 2a PE 5.8 62.6 60.8 4 0.0 56.9) “O.2 Sova | (1.6 59.0 2.0 3-8 60.6 60.0 ais —o.1 56.7. 0.0 5725 (O89 58.2 Tez 2.0 58.8 59.0 ee —o.1 56.5 —0.2 $7.4 078 Ay pe dae ARS 1.3.6.5 58.6 fo) .- 0.1 56.0 —o.7 S703 0.7 57.0% 0.0, =0.1 56.7 57.4 —0o. -—O.1 55.7 —I.0 47 A ails Dy f 56.0 —1I.0 —I.4 55.4 56.8 —t1 - —0.2 55.1 —1.6 5a TO. 0 54.9 —2.I1 —3.3 53.5 55-4 —2 : 0.0 54.7 —2.0 57.0 0.4 53.8 —3.2 —4.8 52.0 54.6 —3 0.2 54-3 —2.4 56.1 —0.5 52.9 —4.1 —6.8 50.0 53-2 —4 0.0 bene OF 55.6 —1.0 52.7 —4.3 —6.0 50.8 52.7 —4 0.3 lasis O68 55.6 —1.0 52.8 —4.2 —5.4 51.4 52.7 —3 0.2 —0.3 55.6 —1.0 2.8 —4.2 —5.3 51.5 52.7 —3 0.2 —o.1 55.6 —1.0 2.8 —4.2 —5.1 51.7 52.7, ——8 0.0 0.0 55-3 —I1.7 52.8 —4.2 —5.9 50.9 52.7 —4 - —O.1 0.0 54.8 —1.6 52.8 —4.2 —5.7 51.1 52.6 —4 .-—0O.1 0.3 54-7 —I.9 52.9 —4.1 —5.8 51.0 52.6 —4 -—0.1 0.9 54.5 —2.1 53-2 —3.8 —5.1 51.7 52.5 —3 . —O.1 1.2 54.6 —2.0 53-1 —3.9 —4.8 52.0 52.5 —3 - —0.2 ri5 55.0 —1.6 53.9 —3.1 3,453.4 52.6 —2 5 0.0 1.5 55-4 —I.2 54.0 —3.0 —2.7 54.1 53.0 —I 0.1 “scp 55.6 —1.0 54-1 —2.9' 2.1 54.7 53.2 —I ORR AHOHK AN OD OAWOHORUHHAROCRUHA HUA OOM — BORR HN OND 13 TABLE 3.—Continued 186,400 122,900 PERIODS RELATED TO 273 MONTHS—ABBOT ir 61,400 f : M NO. ean Periods nm years PS, O}O0) Eee RE ENING YESS RUN 560 SOUS CO)-S TEN CUES AICO INS BS BOND SESE OO OD UN 9 NO NOE CI B3] BOO NS ARISES EC OO EN ISAC ESS GES Co EN SRO IND DIMIAMGCCS PRAACOSCOCACOHHAHODADNROSONTMMAHANAAAMOMTMMSRRROOH ROO MMM RRRO MUMOMMMMMMMMMMMMOOOO MOWOOCOOOO MMMM NMHNH NNN MMNMNNNMNHMNNNMHNMHNMHMNM MMMM nwMnnnNMwy MODOKHHTFHHODH ATO TOHOONATAMODAKND THTOSOADMANMANMAH ONO TOMO RNR MMA MH NOH MO HOC own el wt a elles Mee wise oe One, i ei e Ke aah s)he Mb cetin le fas. aia ay ws LN Seka Onan eras) vel oe! ee) LOL ince mee ce" ce) Lele kin ame eee ee awn te Vo ya ie he er een cl na a) Cs gayi fa acon ase my egret | | flash hte aie thane leat taht a tae ep tee 28)" 8 le se) Ta ey ime ee al8).- 0 Kin KO: UR NS) sen 8. MAW a iw ak “a Sim) ries es Meee ate, oe! (Be poe oe a TTMOMNMTPMMMOMNNMOOHANHHHAMMEANMNAROANOMMNAHOAOCOKHANAN MTOM NOOO AO BRO MMMN +t tO RNC MMMM M MM MMM MMOOUWWOUOOWUOWOUWOWOWOUWOUOWOO HNN NHMH HHH TMM NHN HHH HNN HN HHH KH HNN NMHNMNNNHMNMwM NOPTMMOMOKHHMMMNOATPAH MNO MOOR ATNAOMMTAHHTTONOMNTMHMOOTTOHARMNMNO TMA MIND HA aa mak LK Jk la ies 0 ain Wa i ee Oe Ol We om Gt alee al cee “Ti deel as De aa oom i sl Vs dee lee gtd we ew fb ota ey bee eye et ee ee COHHNNHOOHRHHANNHORM Hah seereeeiae Foilstetlealea Te rE Gs te ee: \SCler eet: aed eure) Eee el ERE Eee ee a we es TES, T'S Ee Sue) eles Mw Nie y teins» fe PON se) St AO lle Pn ENO GR iid el iO Ow LS eS 8) Che Aca ee SiC ces Soe ce 7 [label SEtclet ala iel ale eee ome oe (ape a p) 6Gee cos a8 ese apis o) 6 ng a. «et aye OCR MN es, 6h ce « (ec aiy J Jodie se 6) wie 8) 6 TON A: tee gems 6. Cmrom sine meee Hp5 74 HMM ODOCOOFHHANANANNNHOQOCOCOCOC OH HHH Ne MANN Re OOO OOM HH ANANNNMODOCOCOCON MN eee TTTTTTT ETT TTT TTHT laa er peces te ta Me te Gry Pape s donate des ete os oe ty ee Se aren eat Be Ae ees SE FIRS BE S| Seine RR ee PR Seas Be age TRB PSS Oo Soe Pe Pets bei a+ : PEEP EH! Lhidtind } aes Fe Es a eet ed Se IGE ES Pe er a ape ge oe ae toa SSR eee gs a ngs MOREE SH bie i IER 2 5 ies $s i ae Os tee a nt UT es EE BR A eae ie Maks Siete yi te AR CS hed beh Se ae tilt so gee ee ie ee al a @ iile go: je wie. ete. a ee ew. eee Se) 8 Cw Te” eee eee bee ie 8 | lee ey mee Ee OMe KON! “e." a>, 6 Se) mate mee Cig s UmRAe (emo) ieee eee) ew aes He ee Li oe sees eee weer eceee eee eeee were eens ae eeee eres ewes . eens ewer eaee coer . oe wees weer eee eeee . eeee . eens seen and finally . ’ Mean 56.8° then curve B, . ’ In figure 6 I plot the smoothed Soergel curve A 245.8 thousands of years, and the departures of each of these mean which is the synthesis of my four long periods plus 56.8° curves from the general mean for each. 14 a) SMITHSONIAN MISCELLANEOUS COLLECTIONS HAIGIina reneR TTT TRL CEE LITEREERERRUTAGISE HALENEMERLIS HINHERERADD> canal EL ber TTT en = 10 gen. B, Synthesis of four periods, multiples -of 273 C, Curve B reduced to “%o in ordinates. months, Fic. 6.—Glacial penetration in Germany. A, Soergel’s curve as smoothed by Griinha No. I PERIODS RELATED TO 273 MONTHS—ABBOT 15 curve C, which is my synthesis multiplied by %o plus 56.8°. It is plain that the principal features and even most details of the smoothed Soergel curve are closely duplicated in my curve C. As Griinhagen used 6 periods, and I used but 4, the scale difference, 10 to 7, may be for lack of the others. I do not fully understand how Soergel derived the time scale for these very ancient events. Doubtless he used several disciplines, in- cluding paleontology and stratigraphy. It is extraordinary how closely my exact time scale fits with his time scale, which must have been built up from rather loosely timed data. 4, MAGNETIC AND ELECTRICAL RELATIONS TO THE PERIOD OF 273 MONTHS Nearly 50 years ago Dr. G. E. Hale discovered magnetism in sun- spots. When this phenomenon had been followed long enough, the well-known remarkable reversal of polarities at intervals of double the sunspot period of 11% years was found. So the 273-month period is surely a magnetic period in the sun. When, about 1935, the ionosphere became systematically observed, the fluctuation of these electrical phenomena proved to be closely associated with sunspot frequency. But later I discovered that iono- spheric changes were also associated with the variations of measures of the solar constant. I will merely refer here to publications on this relationship.® 5. THE HUMAN PULSE RATE In a former publication 1° I mentioned that my friend Dr. F. P. Marshall had kept a record of her pulse rate for three years, which indicated a regular period of 212 days and submultiples thereof. The observations were made every day before rising, and form a continu- ous record for 1,095 days of basal pulse rates. Dr. Marshall has kindly permitted me to use this evidence, which is unpublished. It shows clearly a period of 212 days and six periods, aliquot parts thereof (fig. 7), and others which I have not investigated. Dr. Marshall was familiar with my first studies on the solar constant of radiation, about 1935. She followed much the same course with the pulse observations. However, as the 15-year record of solar- ® Smithsonian Misc. Coll., vol. 107, No. 4, pp. 24-26, 1947; ibid., vol. 122, No. 4, Pp. Q-II, 1953. 10 Periodic solar variation, Smithsonian Misc. Coll., vol. 128, No. 4, pp. 3, 6, 1955. 16 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 constant measures then available had many breaks in the continuity of the daily observations, I was constrained to use 10-day and monthly Po eee a ee eee te Ly Le | een a oe Mme eee te ls Sl ee HR in eA ete at ated bot pe de, ake ae a De ee 2aal | | Som ae lee a S wee oe Lt, TA ye fe tesa Ss dea A A BY mer se De ir Fat A n= ea A, cl er AA ACR ate eves lesen ved Sheltie. EE Mo Vd Fic. 7—Basal pulse rates (Marshall). A, Mean march of 212- day period for 3 years. D, Period of 74% removed. E, Period of 2% removed. B, Period of 21% removed. C, Period of 74% removed. F, Period of 22%1 removed. G, Remain- ing period of 21347, not removed. Seven months, 89 X 273 months, is 213.07 days. Therefore all seven periods found are submultiples of 273 months. mean values in my work. As she had an unbroken daily record of almost 1,100 days, she employed daily values of pulse. Plotting these in their complete continuity, her figure, like my solar- constant figure, resembled a wide ribbon, with its many closely lying ups and downs. But the pulse values, not being subject to accidental errors, were more satisfactory to investigate than the solar-constant values in which accidental errors were of about the same magnitude NO: I PERIODS RELATED TO 273 MONTHS—ABBOT 17 as real variations of the sun. Still her ribbon plot was so wide that it was found desirable to smooth the record. This she did by taking 7-day overlapping means. The range of pulse remaining after smooth- ing was approximately from 60 to 70 pulses per minute. Scanning the smoothed pulse record, it appeared to present a re- curring period of 106 days. The range of that period seemed to show alternately maxima and minima. So a period of 212 days was sought for by tabulation. With five repetitions of the 212-day tabulation, their mean was as represented by the hne A in figure 7. It is easy to see that, though loaded with many irregularities, the line A is fairly indicative of an approximate sine curve, with a range of two pulses, as shown by the smooth line. Following the procedure of my weather-variation papers, the curve A was cleared successively of five periods, which are aliquot parts of 212 days, respectively %4, 44, %, %, and 41 of 212 days. These are shown in the upper part of figure 7. The successive removals of them show the successive smoothing of curve A, in curves D, E, B, C, and F. There still remains, as shown in curve G, a period of = days, or 12% days, and doubtless others. But curve F is so smooth that little doubt remains that the smooth line upon curve F is the veritable period of 212 days, as relieved of superriders. This smooth line is almost exactly the same in form and amplitude as that drawn free-hand on curve A. It has a range of two pulses or about 3 percent of the aver- age pulse rate per minute. In the solar variation, a 7-month period is one of the stronger ones. Reduced to days, a 7-month period is %9x 22% years, which is 22-75 X 305-2504 _ 9, 3.07 days. This, of course, to well within the probable error, is the same as Dr. Marshall’s 212 days. Hence I con- clude that Dr. Marshall’s physiological period and its exact submulti- ples are all aliquot parts of my master solar period of 273 months. Doubtless this relationship is not accidental, and physiologists will, I am sure, note it with interest. SUMMARY The author shows that weather, glaciation, dates of snow coverage in Japan, magnetism in the sun, variations of the ionosphere, and human pulse rates all present regular periods which are exact multi- ples or submultiples of the master period of 273 months in the varia- tion of the sun’s emission of radiation. -SMITHSONIAN MISCELLANEOUS COLLECTIONS VOLUME 134, NUMBER 2 THE ASIATIC SPECIES OF BIRDS OF THE GENUS CRINIGER (PYCNONOTIDAE) By H. G. DEIGNAN Associate Curator, Division of Birds U. S. National Museum Smithsonian Institution o? MEINC A ney ORS ERAN Su eZ ° os, . AGN THSO NOD ob See A NGTOM See oe2 (Pusication 4266) CITY OF WASHINGTON PUBLISHED BY THE SMITHSONIAN INSTITUTION OCTOBER 25, 1956 THE LORD BALTIMORE PRESS, INC. BALTIMORE, MD., U. S. A. Pat ASIATIC SRBCins. OF BIRDS OTHE GENUS CRINIGER (PYCNONOTIDAE) By H. G. DEIGNAN Associate Curator, Division of Birds U. S. National Museum Smithsonian Institution Among the birds of tropical Asia, few groups can have been the subject of so many revisions with such diverse results as the forms of the pycnonotine genus Crimiger. In the course of studies made in connection with work on the bulbuls for the continuation of the late J. L. Peters’s “Check-list of Birds of the World,” I have found that there has been no agreement among the several authors even as to the number of species involved, and it has frequently proved quite impossible for me to decide which form was meant by a name used in a particular instance. In the circumstances, I have been compelled to make a wholly new study based upon personal examination of hundreds of specimens and of many of the pertinent types, and here present a new arrangement that will, I believe, settle most of the previously doubtful points of relationship within the group. Six species (five of them polytypic) are accepted, each of which appears to be somewhere sympatric with one or more of the others, but in the pages to follow will be found no comment on the two uncontroversial species, finschii Salvadori, 1871, and phaeocephalus (Hartlaub), 1844. CRINIGER FLAVEOLUS (Gould), 1836 Criniger flaveolus flaveolus (GouLD). Trichophorus flaveolus Goutp, Proc. Zool. Soc. London, pt. 4, No. 37, April 0, 1836, p. 6 (‘“‘ in montibus Himalayensibus, in Nepalia, «c.”; type locality restricted to Nepal, by Koelz, Contr. Inst. Reg. Expl., No. 1, 1954, p. 10). Trichophorus xanthogaster Hovcson, in J. E. Gray, Zoological Miscellany, No. 3, “June” 1844, p. 83 (Nepal). Nomen nudum. Lanixus xanthogaster “Hodgs.” BowpLer SHARPE, Catalogue of the Birds in the British Museum, vol. 6, 1881, p. 77 (Nepal). In synonymy with Criniger flaveolus (Gould), not Criniger xanthogaster Cassin, 1855. Trichophorus xanthogaster “Hodgs.” BowDLerR SHARPE, Catalogue of the Birds in the British Museum, vol. 6, 1881, p. 77 (Nepal). In synonymy with Criniger flaveolus (Gould), not Criniger xanthogaster Cassin, 1855. SMITHSONIAN MISCELLANEOUS COLLECTIONS, VOL. 134, NO. 2 2 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 Criniger flaveolus viridulus Kortz, Contr. Inst. Reg. Expl., No. 1, Septem- ber 24, 1954, p. 10 (Sangau, Lushai Hills, Assam State, India). Criniger flaveolus aureolus Koetz, Contr. Inst. Reg. Expl., No. 1, Septem- ber 24, 1954, p. 10 (Kohima, Naga Hills, Assam State, India). Range.—The sub-Himalayas from Garhwal to easternmost Assam, south through Assam to Arakan, the Chin Hills, central and north- eastern Burma. Criniger flaveolus burmanicus OarTEs. Criniger burmanicus Oates, Fauna of British India, Birds, vol. 1, Decem- ber 1889, p. 256 (““Toungngoo; the Karen hills; Karennee; Tenasserim, as far south as Meetan at the base of Muleyit mountain, and throughout the Thoungyeen valley” ; type locality commonly restricted to Toungoo District, Pegu Division, Burma). Range.—Southeastern Burma (the valley of the Salween from the Northern Shan States to its mouth in the Amherst District of Tenas- serim) and western Thailand (valleys of the Mae Moei [Thaungyin] and the Mae Klong). Remarks.—Criniger flaveolus burmanicus seems to be sympatric in central Tenasserim with Criniger pallidus robinsoni and Criniger ochraceus ochraceus, and in southwestern Thailand with Criniger ochraceus ochraceus. CRINIGER PALLIDUS Swinhoe, 1870 Criniger pallidus pallidus SwinHoe., Criniger pallidus SwinHok, Ibis, ser. 2, vol. 6, No. 22, April 1870, p. 252 (Hainan). Pinarocichla schmackeri Styan, Bull. Brit. Orn. Club, vol. [1], No. ap November 1, 1892, p. vi (Hainan). Range.—Hainan. Criniger pallidus henrici OusTAtet. Criniger Henrici Oustater, Bull. Mus. Hist. Nat. [Paris], vol. 2, No. 5, June 22, 1896, p. 185 (“entre Manhao et Se-mao [Yunnan], sur les bords de la Riviére-Noire . . . A Nam-Xong, Ban-Moi et Hat-Hoa [Tonkin]’’). Crimger pallida grandis Stuart Baker, Bull. Brit. Orn. Club, vol. 38, No, 228, December 4, 1917, p. 15 (Yunnan Province, China; type specimens from Yuankiang [lat. 23°37’ N., long. ro2°or’ E.]). Range.—Southern Yunnan (valleys of the Red and Black Rivers), Tongking, northernmost Annam, northwestern Laos, Southern Shan States (valley of the Mae Khong), and northern Thailand. Criniger pallidus robinsoni Ticreuurst. Criniger tephrogenys robinsoni Ticeuurst, Bull. Brit. Orn. Club, vol. 53, No. 362, October 31, 1932, p. 19 (Ye, Amherst District, Tenasserim Division, Burma). NO. 2 ASIATIC BIRDS OF GENUS CRINIGER—DEIGNAN 3 Range.—Southern Burma (the Amherst District of Tenasserim) and (probably) northwestern Thailand. Remarks.—This form was based upon three faded specimens in London, collected in the Amherst District during the 1870's; two of them, including the type, are apparently immature, differing from an obvious adult by paler, bright, and more gold-suffused coloration above and below, and by the slight development of the gular feathers. The length of crest feathers and tail of the adult show that it be- longs rather with pallidus than with bres (“tephrogenys”’ of Tice- hurst), and making allowances for its quite serious fading, it appears to represent a population intermediate between henrici and griseiceps. An apparent difficulty arises from the fact that griseiceps is until now reported only from the Pegu Yomas, robinsoni only from the Amherst District of Tenasserim, and henrici from nowhere south and west of Doi Ang Ka (lat. 18°35’ N., long. 98°30’ E.) in northwestern Thailand ; thus the three populations seem to be quite isolated from each other. Yet it is difficult to believe that the intervening territory, so suitable for the species, should wholly lack some representative of the group, and the suspicion that the vacuum is more imaginary than real is supported by the existence of a unique skin (M.C.Z. No. 196535) from Doi Ang Ka that can be separated from griseiceps only by having the crest feathers colored quite as in henrici, without the least grayish wash. A second indication of probable intergrada- tion between the two, and one further strengthening the view that robinsoni is an intergradient population, is the fact that, of the two faded paratypes of robinsoni now before me in Washington, while the adult has the crest faintly washed with gray (as if approaching griseiceps), the immature has it red-brown (as if approaching henrici). For the present, I consider griseiceps a geographically and chromat- ically extreme representative of Criniger pallidus, with which it is connected in conventional fashion through robinsoni. Criniger pallidus robinsoni seems to be sympatric in the Amherst District with Cringer flaveolus burmanicus and Criniger ochraceus ochraceus. Criniger pallidus griseiceps Hume. Criniger griseiceps Hume, Stray Feathers, vol. 1, No. 6, December 1873, p. 478 (“Upper Pegu,” Burma). Range.—Southern Burma (Pegu Yomas). Remarks.—This race is very strongly marked compared with others of the species. Its mantle is greener (but wholly lacking the golden tone appearing in Criniger fl. burmanicus) ; its crest is strongly suf- fused with gray, although basically a dull red-brown as in the rest. 4 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 Another peculiarity is its suffusion of pinkish buff, which affects the throat, the ground color of the under parts, and the tones of the crest and upper parts, but a similar suffusion appears in slight degree also in some skins of henrici from western Thailand. In the circumstances, and because of the specimen from Doi Ang Ka discussed above, griseiceps seems to be properly placed in the species pallidus. Criniger pallidus isani, subsp. nov. Type.—U.S.N.M. No. 459700, adult male, collected at Ban Muang Khai (lat. 17°30’ N., long. 101°20’ E.), Loei Province, Thailand, on January 14, 1955, by Robert E. Elbel; original number RE 4470. Diagnosis —Nearest Criniger pallidus henrici, from which it is separable by having the olivaceous brown of the mantle decidedly paler and grayer. Range.—Eastern Thailand (Loei and Phetchabun Provinces). Remarks.—Although no representative of the genus had previously been reported from the Phaya Dong Fai Mountains, I have recently acquired no fewer than 24 specimens of this new race from several localities in the northwestern portion of the eastern plateau of Thai- land, and the bird will certainly be found to possess a much more extensive range. Criniger pallidus annamensis DELACoUR AND JABOUILLE. Criniger tephogenys annamensis DeELacour AND Jaxourtie, Bull. Brit. Orn. Club, vol. 45, No. 291, December 5, 1924, p. 32 (Lao Bao, Quangtri Province, Annam). Range.—Central Annam, intergrading in northern Annam (Phu Qui) with henrici, and in south-central Annam (Dak To, Kontoum) with the next following race; central Laos, from Chiang Khwang southeastward to Lao Bao. Criniger pallidus khmerensis, subsp. nov. Type—U.S.N.M. No. 360999, adult male, collected at Banteai Srei (lat. 13°16’ N., long. 104°07’ E.), Siem Reap Province, Cam- bodia, in January 1940, by Joseph F. C. Rock; original number 1292A, Diagnosis.—Nearest Criniger pallidus annamensis, but separable by the brighter, more purely yellow (less buff-suffused) under parts and the much more golden-olive (less brownish-olive) mantle. Range.—Southern Annam (Phanrang and Haut-Donai Provinces), Cambodia, and southern Laos (Saravane Province). Remarks.—Criniger pallidus khmerensis seems to be sympatric in southern Annam with Criniger ochraceus subsp. nov. (named just below). NO. 2 ASIATIC BIRDS OF GENUS CRINIGER—DEIGNAN 5 CRINIGER OCHRACEUS Moore, 1854 Criniger ochraceus hallae, subsp. nov. Type.—Brit. Mus. Reg. No. 1928.6.26.834, adult male, collected at Tay Ninh (lat. 11°18 N., long. 106°07’ E.), Tay Ninh Province, Cochin-China, on January 15, 1928, by Jean Delacour and Willoughby P. Lowe (Franco-British Indo-China Fourth Expedition) ; original number 1767. Diagnosis.—Nearest Criniger ochraceus cambodianus, from which it differs by having the mantle less grayish, more strongly suffused with olivaceous, and the under parts much brighter, strongly suffused with creamy- or yellow-buff. Range.—Southern Annam (Haut-Donai Province) and Cochin- China (Bien Hoa and Tay Ninh Provinces). Remarks.—This isolated population (named for Mrs. B. P. Hall of the British Museum, Nat. Hist.) has until now been placed with the nominate race of Tenasserim, from which it is of course quite distinct. It is apparently sympatric in southern Annam with C: riniger pallidus khmerensis. Criniger ochraceus cambodianus DELACOUR AND JABOUILLE. Criniger gutturalis cambodianus DELAcoUR AND JABourLie, Bull. Brit. Orn. Club, vol. 48, No. 325, July 10, 1928, p. 130 (Le Boc Kor [lat. 10°37’ N., long. 104°03’ E.], Kampot Province, Cambodia). Range.—Southwestern Cambodia (Chaine de VEléphant) and southeastern Thailand. Criniger ochraceus ochraceus Moore. Criniger ochraceus Moore, in Horsfield and Moore, Catalogue of the Birds in the Museum of the Hon. East-India Company, vol. 1, 1854, pp. xv Lxomen nudum], 252 (Tenasserim Division, Burma; type locality here restricted to Mergui [lat. 12°26’ N., long. 98°36’ E.], Mergui District). Criniger ochraceus crinitus DEIGNAN, Journ. Washington Acad. Sci., vol. 44, No. 4, May 3, 1954, p. 125 (Ban Hin Laem [lat. 14°40’ N., long. 98°40’ E.], Kanchanaburi Province, Thailand). Range.—Tenasserim from the Amherst District (Ye) south to the Mergui District (Tenasserim Town), and southwestern Thailand (valley of the Mae Klong and south in the forest to Prachuap Khiri Khan Province [Khao Luang]). Remarks.—Since two races of ochraceus appear in Tenasserim, it has been necessary to restrict Moore’s type locality. Comparison of the type specimen in London with others has shown that nominate ochraceus occurs as far south as Tenasserim Town, and one specimen from that place is even very like the type itself in its deep coloration. 6 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 Accordingly, Mergui, still farther north and the provenience of a number of Helfer’s skins, may be considered a suitable terra typica. Criniger ochraceus ochraceus seems to be sympatric in central Tenasserim with Cringer pallidus robinsoni and Criniger flaveolus burmanicus, and in southwestern Thailand with Criniger flaveolus burmanicus. Criniger ochraceus sordidus RICHMOND. ?Criniger Cabanisi A. MULLER, Die Ornis der Insel Salanga, [ante October 4] 1882, p. 32 (Phuket [lat. 7°55’ N., long. 98°25’ E.], Phuket Province, Thailand). ?Criniger Cabanisi A. Mixxer, Journ. fiir Orn., Jahrg. 30, No. 160, November 1882, p. 384 (Phuket, Phuket Province, Thailand). Criniger sordidus R1cuMonpD, Proc. U.S. Nat. Mus., vol. 22, No. 1201, May 12, 1900, p. 320 (Khao Soi Dao [lat. 7°20’ N., long. 99°50’ E.], Trang Province, Thailand). ?[Criniger] salange BowpvLerR SHARPE, Hand-list of the Genera and Species of Birds, vol. 3, 1901, p. 316. New name for Criniger Cabamsi A. Miller, Journ. fiir Orn., Jahrg. 30, No. 160, November 1882, p. 384 (Phuket, Phuket Province, Thailand), not Criniger cabanisi Bowdler Sharpe, “1881” [1882]. Range.—The Mergui Archipelago (Ross, Sullivan, and St. Mat- thew’s Islands) and mainland Tenasserim from the head of Pak Chan Estuary to Victoria Point; Thailand from Sathani Map Ammarit (lat. 10°50’ N., long. 99°20’ E.) south through the Malay Peninsula into northwestern Malaya (Perlis State and the Langkawi Islands). Remarks.—Criniger ochraceus sordidus has lain in synonymy with the nominate race for many years, but it is readily distinguished in series by its darker upper parts and more ochraceus, less buffy, under parts. Most discussion of this form has been based upon skins from the Merguis and Tenasserim and from the Siamese side of the Isthmus of Kra, all of which are, strictly speaking, sordidus>ochraceus, and therefore misleading for taxonomic purposes. This form is apparently sympatric in southernmost Tenasserim, peninsular Thailand, and northwestern Malaya with Criniger bres tephrogenys. Criniger ochraceus sacculatus Ropinson. Criniger ochraceus sacculatus RoBINson, in Robinson and Boden Kloss, Ibis, ser. 10, vol. 3, No. 4, October 8, 1915, p. 746 (Ginting Bidei [lat. 3°18’ N., long. 101°50’ E.], Selangor State, Malaya). Range.—Malaya, from northern Perak south to Negri Sembilan and Pahang. Remarks—Criniger ochraceus sacculatus is apparently sympatric in Malaya with Criniger bres tephrogenys. It is frequently stated that the former is a hill form, while the latter is one of the lowlands, NO. 2 ASIATIC BIRDS OF GENUS CRINIGER—DEIGNAN 7 but it should be noted that sacculatus ranges principally between 2,500 and 4,500 feet, while tephrogenys “is met with on the hills of Negri Sembilan, and on Kedah Peak, and also on the hills of Patani up to about 3000 feet” (Robinson, Birds of the Malay Peninsula, vol. 2, 1928, p. 163). Both forms have been taken at Ginting Bidei at an elevation of 2,300 feet. Criniger ochraceus sumatranus WARDLAW RAMSAY. Criniger sumatranus WarpLAw Ramsay, Ann. and Mag. Nat. Hist., ser. 5, vol. 10, No. 60, December 1882, p. 431 (“M[ount]. Sago” [ca. 70 miles northeast of Padang, which lies at lat. 0°58’ S., long. 100°21' E.], Sumatra). Range.—Highlands of western Sumatra. Criniger ochraceus ruficrissus BowpLER SHARPE. Criniger ruficrissus BowpLeR SHARPE, Proc. Zool. Soc. London, for 1879, pt. 2, August 1879, p. 248 (Kina Balu [lat. 6°05’ N., long. 116°30’ E.], North Borneo). Range.—Highlands of northern Borneo. Remarks—Although some authorities prefer to treat ruficrissus as a monotypic species, I look upon it as merely a strongly marked geographical representative of ochraceus. It is apparently sympatric in northern Borneo with Criniger bres gutturalis (see Finsch, Notes from the Leyden Museum, vol. 26, 1905, p. 106). CRINIGER BRES (Lesson), 1832 Criniger bres tephrogenys (JARDINE AND SELBY). Trichophorus tephrogenys JARDINE AND SELBY, Illustrations of Ornithology, ser. I, vol. 3, pt. 9, February 1833, pl. 127 and text (“. . . though we are uncertain of its locality, we suspect it to be Indian”; type locality corrected to Malacca, by Hartert, Nov. Zool., vol. 9, 1902, p. 558). Range.—Southern Tenasserim (one specimen from the Mergui District in Liverpool, ex Coll. Tristram) ; peninsular Thailand south- ward from the Isthmus of Kra; Malaya; lowlands of eastern Sumatra. Remarks.—Criniger bres tephrogenys is apparently sympatric in southern Tenasserim and peninsular Thailand with Criniger och- raceus sordidus, and in Malaya with Criniger ochraceus sacculatus. Criniger bres gutturalis (BONAPARTE). Tlrichophorus\. gutturalis “Mull. Mus. Lugd.” Bonaparte, Consp. Gen. Av., vol. 1, 1850 or 1851, p. 262 (Borneo type specimen from Banjermasin [lat. 3°20’ S., long. 114°35' E.], fide Finsch, Notes from the Leyden Musuem, vol. 26, 1905, p. 105). Range—Borneo. Remarks.—This form is apparently sympatric in northern Borneo with Criniger ochraceus ruficrissus (see Finsch, loc. cit., p. 106). 8 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 Criniger bres frater BowDLER SHARPE, Criniger frater BowbLer SHarre, Trans. Linn. Soc. London, ser. 2, vol. i pt. 6, November 1877, p. 334 (Puerto Princesa, Palawan Island, Philippine Islands). Range.—Palawan. Criniger bres bres (Lesson). Turdus gularis HorsFieLp, Trans. Linn. Soc. London, vol. 13, pt. 1, May 1821, p. 150 (Java). Lanius Bres Lesson, in Bélanger, Voyage aux Indes-Orientales, pt. 4, August 1832, p. 255 (Java; type locality here restricted to Bogor [Buitenzorg] ). New name for Turdus gularis Horsfield, Trans. Linn. Soc. London, vol. 13, pt. 1, May 1821, p. 150 (Java), not T[wrdus]. gularis Latham, 1801. Trichophorus xanthizwrus OBERHOLSER, Smithsonian Misc. Coll., Quarterly Issue, vol. 48, No. 2, July 1, 1905, p. 152. New name for Turdus gularis Horsfield (vide supra), not T[urdus]. gularis Latham, 1801. Criniger balicus bartelsi Covtin AND Hartert, Nov. Zool., vol. 34, No. 1, August 10, 1927, p. 51. New name for Turdus gularis Horsfield (vide supra), not TLurdus]. gularis Latham, 1801. Range.—Western and central Java. Remarks.—Since two forms of the species are known from Java, it is important to know which one is represented by Lesson’s type specimen. Bélanger (Voyage, pp. Xxix-xxx) says: “. . . j’entrepris, . un nouveau voyage aux iles de la Sonde. Le détroit de ce nom, une partie de la cote orientale de Java, les districts de Bantam et de Buitenzorg dans cette ile, furent les lieux principaux soumis a mes recherches.” In short, Bélanger’s collections were made within the ranges of both races. It is no longer possible to solve the problem by examination of Bélanger’s material. In reply to my query, Professor Berlioz has written: “I am sorry to say definitely that we do not possess this type of Lesson nor any bird which might be eventually considered as such. In fact there are extremely few birds here originated in Bélanger’s travel—and in very bad condition—and if ever this bird came to our Museum it is not impossible that it would have been destroyed, as there is no trace of it even in our old register.” 2 In the circumstances, I am justified in fixing a type locality for Lesson’s bres, and have chosen Bogor (Buitenzorg) as a place visited by Bélanger and one at which commonly occur birds clearly assignable to the more western race. Criniger bres balicus StTRESEMANN. Criniger gularis balicus STRESEMANN, Nov. Zool., vol. 20, No.2, June 17, 1913, p. 358 (Gitgit, Bali Island). Range.—Eastern Java ‘and Bali. NO. 2 ASIATIC BIRDS OF GENUS CRINIGER—DEIGNAN 9 ACKNOWLEDGMENTS For the loan of valuable material used in this study, I am greatly indebted to the authorities of the British Museum (Nat. Hist.), Lon- don, the Museum of Comparative Zodlogy, Cambridge (Mass.), the American Museum of Natural History, New York, the Chicago Natural History Museum, and the Academy of Natural Sciences of Philadelphia. For information and advice on specific problems, I owe thanks to Professor J. Berlioz of the Museum at Paris, to Mrs. B. P. Hall of the British Museum, and to Charles H. Rogers of the Princeton Museum of Zoology. Nee eee eS: aaa SMITHSONIAN MISCELLANEOUS COLLECTIONS VOLUME 134, NUMBER 3 Charles BD. and Mary Waux Walcott Research Fund BOOP DEVELOPMENT OP THE PENNSYLVANIAN TEREBRATULID CRYPTACANTHIA (WitH 2 Piates) By G. ARTHUR COOPER Head Curator, Department of Geology United States National Museum Smithsonian Institution (PusiicaTion 4267) CITY OF WASHINGTON PUBLISHED BY THE SMITHSONIAN INSTITUTION JANUARY 31, 1957 THE LORD BALTIMORE PRESS, INC. BALTIMORE, MD., U.S. A. Charles B. and Mary Waux Walcott Research Fund LOOP DEVELOPMENT OF THE PENNSYLVANIAN TEREBRATULID CRYPTACANTHIA By G. ARTHUR COOPER Head Curator, Department of Geology United States National Museum Smithsonian Institution (WitH 2 PLatTEs) The silicified specimens forming the subject of this discussion are unusual in preserving parts or all of the internal skeleton in youthful individuals as well as adults. They were dissolved from Magdalena limestone taken from a ledge on the north side of an arroyo just east of the Grapevine Canyon road one-eighth mile south of Old Juniper and a cattle tank, about in the center of the W4SE4SW435 sec. 25, T. 19 S., R. 11 E., Escondido Canyon (15’) Quadrangle, Otero County, N. Mex. These fossils and others described earlier from the same place (Cooper, 1956) are from 30 to 4o feet below the top of the Magdalena formation. The bed containing these fossils is a gray, fine-grained limestone containing a large amount of light-gray insoluble material and nu- merous other brachiopods, among which are: Cleiothyridina, Puncto- spirifer, Stenoscisma, Dielasma, and smaller forms still to be identified. Immature forms of several of the genera are very abundant and some small specimens appear to be adults of an undescribed genus. Gas- tropods and pelecypods are fairly common but their preservation is poor. One of the most abundant brachiopods in this limestone is the hitherto poorly known and extremely rare genus Cryptacanthia. Al- though this genus has been identified in many areas of Pennsylvanian rocks, it is one of the rarest of all Pennsylvanian fossils. The origi- nal specimens on which the genus was based come from Iowa but it is known in adjacent Illinois and Missouri. It occurs in the Gaptank formation in west Texas and is known elsewhere in New Mexico and Kansas besides the occurrences mentioned above. The genus was de- SMITHSONIAN MISCELLANEOUS COLLECTIONS, VOL. 134, NO. 3 2 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 scribed by White and St. John (1867) but little has been written about it since then. Dunbar and Condra (1932) redescribed the genus and added another species from the early Permian. Study of the specimens described herein and of another preparation of the loop of Cryptacanthia from Madison County, Iowa, shows that this struc- ture was improperly restored by Dunbar and Condra. About a dozen blocks of various sizes were collected at the locality in Grapevine Canyon. These yielded about 4,000 specimens of Cryptacanthia, including many with almost perfect interiors and some with the loop preserved to perfection. These specimens permit a nearly complete description of the development of the loop and other details of the interior. This is the first Paleozoic long-looped brachio- pod in which the stages of loop development have been described. In comparing the New Mexico specimens with those from Iowa, which are topotypes, it was discovered that the ones from the South- west are clearly a new species for which the name Cryptacanthia pro- lifica Cooper is here proposed. CRYPTACANTHIA PROLIFICA Cooper, new species Small, pentagonal in outline, length and width nearly equal but varying from an oval outline in the young to subpentagonal in the adult ; inequivalve, the pedicle valve having the greater depth, postero- lateral margins nearly straight forming an angle at the beak of 105° to 110°; sides narrowly rounded; anterolateral margins gently con- cave to straight; anterior margin truncated to gently emarginate; greatest width at about midvalve but variable with age; anterior com- missure strongly sulcate; surface smooth. Pedicle valve evenly and strongly convex, with the maximum con- vexity at the middle ; anterior profile narrowly domed with steep, con- cave sides ; beak small, incurved, suberect to erect ; foramen elongate- elliptical, mesothyrid to submesothyrid; deltidial plates conjunct; umbo narrow, moderately convex; fold originating on anterior side of umbo, widening anteriorly to front margin, somewhat flat-topped and with a sulcus originating at about midvalve; umbonal slopes gentle, anterolateral slopes precipitate. Brachial valve shallow, evenly and gently convex in lateral profile; anterior profile nearly flat but with a shallow median depression ; umbo gently swollen; sulcus originating just anterior to the umbo, widening and deepening anteriorly to the front margin; sulcus in many specimens with a low, indistinct fold originating just anterior to ——EE — NO. 3. LOOP DEVELOPMENT OF CRYPTACANTHIA—COOPER 3 midvalve and extending to the front margin; flanks bounding sulcus gently convex. Interior.—See Internal Morphology, below. MEASUREMENTS IN MILLIMETERS Brachial Maximum Length length width Thickness FENG EG GIL Lisvsvare’'s 10. Paratype U.S.N.M. No. 127203. Same as preceding but turned to side to show point of echmidium, X 10. Specimen in the 4.1-4.5 mm. stage showing a small but well-formed hood on the point of the echmidium, <8. (See pl. 2, F, fig. 10,) U.S.N.M. No. 127204h. 6. Same specimen as preceding but turned to show elliptical opening of the early-formed hood, X 8. 7. Same specimen as preceding, only slightly turned to the side but showing 8 N mE © the small cuplike hood, X 8. (See pl. 2, F, fig. 11.) . Specimen in the 4.6-5.0 mm. stage showing fully formed and notched hood, 8. Paratype U.S.N.M. No. 127204t. (See pl. 1, I, fig: 27.) 9. Same as preceding but loop seen partially from side, X 8. 10. Specimen in the 3.1-3.5 mm. stage showing incipient hood on tip of echmidium, X 10. Paratype U.S.N.M. No. 1272031. (See pl. 2, D, fig. 7.) Figs. 11, 12, Cryptacanthia compacta: 11. Dorsal view of the loop of Cryptacanthia compacta showing the long spines, deep cleft, jugum, and short descending lamellae. Dotted lines indicate where part of loop was dissolved away but jugum is intact. (Compare pl. 1, A, fig. 1.) Hypotype U.S.N.M. No. 9382a. 12, Same as preceding but showing loop from side with its long spines, prominent erect hood, and long descending lamellae. (Contrast with profile of loop of C. prolifica, pl. 2, H, fig. 16.) 8 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 Stages 1.1 to 1.5 mm.: The smallest specimen (U.S.N.M. No. 127202m) showing traces of the loop is a brachial valve 1.25 mm. long and had a pedicle valve estimated to be 1.50 mm. long. In this specimen only the descending lamella on one side is visible as a thin and delicate ribbon with an angular bend medially at about midvalve (0.4 mm. anterior to the brachial beak). The fact that the descending branch bends medially suggests that at this stage the anterior ends of the loop were united. It is probable that in stages below 1.0 mm. only the initial stages of the descending lamellae are present and are not bent medially at their distal ends. Stages 1.6 to 2.0 mm.: Two specimens (U.S.N.M. Nos. 127202k, 127202n) measuring between 1.5 and 2.0 mm. in length exhibit the loop. Specimen U.S.N.M. No. 127202n is exactly 2.0 mm. long and 1.68 mm. wide. The entire loop is not visible but the pointed anterior can be seen and indicates a loop of about 0.8 mm. in length. The loop of the other specimen (U.S.N.M. No. 127202k) is broken on one side (pl. 2, A, fig. 1) but the descending branches are thin and delicate and bent medially about 0.4 mm. anterior to the beak. These two specimens thus indicate a loop of about 0.8 mm. in length, the lateral branches of which bend medially and unite distally in a sharp point. Stages 2.1 to 2.5 mm.: Information on these stages is based on 5 specimens (U.S.N.M. Nos. 127202-0, p, q, r,s). Three of the speci- mens are 2.4 mm. long and 2.0 mm. wide, but two are 2.3 mm. long and 2.0 mm, wide. The loop varies in length from I.0 to 1.2 mm. The loop is much stouter than in the preceding stage and the crural processes are visible as blunt points. The angular bend of the de- scending lamellae is present and the two branches unite distally to form a sharp, angular, pointed plate not greatly extended anteriorly. The line of junction between the descending branches varies from 0.3 to 0.4 mm. The descending lamellae thus unite to form a spear- shaped plate here called the echmidium.t This name is introduced because, in the development of the loop, the spear-shaped plate be- comes increasingly prominent and ultimately is the site on which grow the ascending elements of the loop. At the 2.1 to 2.5 mm. stages no ascending elements or their beginnings were seen in any of the specimens. Stages 2.6 to 3.0 mm.: Thirteen specimens with this range, hav- ing the loops preserved, appear in the collection (U.S.N.M. Nos. 127202t-z, 127203a-f). The length of the loop averages 1.33 mm. and 1 Echmidium is derived from aichmidion, diminutive of aichme, point of a spear. The ai is transliterated e. NO. 3 LOOP DEVELOPMENT OF CRYPTACANTHIA—COOPER 9 the length of the echmidium averages 0.55 mm. The descending lamellae are thicker and broader than in the previous stages and the bend medially is less pronounced, but the form of the loop is essen- tially the same. The echmidium is broader and longer and now has a long, sharp point. The crural processes are somewhat more pro- nounced and have sharper points than in the preceding stages. Some variation exists in the stoutness of all the elements, but generally they are stronger than the preceding. No ascending elements appear in these stages but traces of them are suspected. In two instances (U.S.N.M. Nos. 127202s, w) a ridge along the center of the ech- midium is suggestive of an incipient development of the hood. Stages 3.1 to 3.5 mm.: Seven specimens in this range preserve the loop (U.S.N.M. Nos. 127202], 127203g-k, 127206k). In these the loop averages 1.48 mm. in length and the echmidium averages 0.65 mm. long. The shortest loop is 1.4 mm. long in a specimen 3.1 mm. long and is 1.6 mm. long in a specimen 3.5 mm. long. This interval sees the appearance of the hood. The best specimen (U.S.N.M. No. 1272031) to show this is about 3.2 mm. long with a loop 1.5 mm. long and with an echmidium 0.8 mm. long which is remarkable for the attenuation of the anterior point and the presence on this point of the first bud of the hood (pl. 2, D, fig. 7). This is 0.56 mm. long measured in the direction of shell length and is 0.24 mm. in height measured at right angles to the length. The line of contact with the echmidium is 0.24 mm. long and is located at the very end of the at- tenuated tip. The delicacy of this structure and its flimsy contact with the echmidium evidently account for the rarity of its preservation. The ventral face of the hood cannot be directly seen but the hood from the dorsal side appears to be elliptical and must therefore form an elliptical opening on the ventral side. From the dorsal side the echmidium shows well the suture between the two descending ele- ments at the line of junction. At the anterior tip of the echmidium a faint trace of divergence laterally of the joined descending and as- cending elements foreshadows the deep cleft in later stages. Stages 3.6 to 4.0 mm.: Five specimens (U.S.N.M. Nos. 127203l, m,n, 0, p) exhibit these stages of the loop, which has become stout, and the echmidium long, wide, and pointed but still undivided. The loop varies in length from 1.6 to 1.8 mm. and the echmidium is 0.88 to 1.0 mm. long. In two specimens (U.S.N.M. Nos. 127203n, 127203-0) the latter plate is 0.60 mm. wide but is still undivided at its anterior tip. Two specimens (U.S.N.M. Nos. 1272031, m) show the hood, the former showing the posterior half (pl. 2, E, fig. 9) and the latter the anterior half. The attachment of the hood to the ech- Io SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 midium is 0.7 mm. long and the hood varies from 0.35 to 0.5 mm. in width. The conical hood tapers rapidly in a posterodorsal direction. Stages 4.1 to 5.0 mm.: Twelve specimens (U.S.N.M. Nos. 127203r-z, 127204c, d, h) in this size range exhibit the loop in vari- ous stages of completeness. The loop varies in length from 2.2 to 2.9 mm. but averages about 2.4 mm. The echmidium varies from 0.8 to 1.8 mm. in length and has a maximum width of 0.64 mm. Specimen U.S.N.M. No. 127204h is 4.8 mm. long and has one of the best pre- served loops in this interval (pl. 2, F, figs. 10, 11). The descending lamellae are broad and flatten anteriorly on the echmidium and be- come nearly vertical. At the anterior end they flare laterally and unite with the lateral walls of the hood. The ventral margin of the hood slopes rapidly posterodorsally, the hood narrowing in that direction. The posterior surface of the hood is short and narrowly convex. Thus in ventral view it expands laterally but with a deep reentrant dorsally. The lateral flaring of the outer walls of the hood is the beginning of the anterior cleft of the echmidium so prominent in succeeding stages. In this specimen the cleft is 0.5 mm. long. The loop at this 4.1 to 5.0 mm. stage is thus an adult one but the anterior cleft is short. The cleft in the anterior point of the echmidium in a smaller specimen (U.S.N.M. No. 127203r) in this range is small and is noticeable only in the hood. The cleavage of the echmidium is thus initiated when the shell has attained slightly more than 4 mm. of length. Specimens of 5 mm. length show a deep cleft in the hood, about I mm. deep in specimen U.S.N.M. No. 127203z. The hood in this specimen is 1.5 mm. long and I mm. wide. Stages 5.1 to 6.0 mm.: Four specimens (U.S.N.M. Nos. 127204k, m, t, u) in this group preserve the loop in most of its details. It is substantially the same as that of the late stages of the previous group but some modifications are evident. The cleft in the echmidium is now deeper, almost half the length of the loop which varies from 3.1 mm. to 3.6 mm. in length. The junction of the lateral branches is short and the reentrant in the hood on the posterior side is deeper in most instances but this appears to be a variable feature. The spines on the anterodorsal side of the loop are long and in two rows anterior to the junction of the lateral branches. The longest spine measures 0.4 mm. in length. The hinge plate in all members of this group is complete and usually perforate. In specimen U.S.N.M. No. 127204t, the loop is 3.6 mm. long, the hood is 1.9 mm. long, the cleft is 1.3 mm. deep, and the hood is 1.2 mm. wide (pl. 1, I, figs. 26, 27; pl. 2, G, figs. 13, 14). Stages 6.1 to 7.0 mm.: Five specimens (U.S.N.M. Nos. 127204-0, NO. 3 LOOP DEVELOPMENT OF CRYPTACANTHIA—COOPER II q, u-w) with loops represent this stage. Anteriorly the lateral branches of the loop are distinctly separated. The hood is 1.6 mm. wide and the posterior surface is long, broadly rounded, and only moderately reentrant. The anterodorsal edge is marked by a double row of fairly strong spines. The loop varies in length from 3.6 mm. to 4.4 mm. and the maximum length of the hood is 2.8 mm. (pl. 2, H, figs. 16-18). Stages 7.1 to 8.0 mm.: One specimen only (U.S.N.M. No. 1272041) in this range shows the loop (pl. 2, I, fig. 19). The speci- men is 7.5 mm. long and 7.2 mm. wide and its loop measures 4.4 mm. in length and the hood is 2.8 mm. long. The anterior spines are long. It is appropriate that at this place the adult loop be described because only one other change in it takes place. The loop of these stages has the crural bases hidden by the com- plete hinge plate which is buttressed against them. The descending branches are short and stout, only 0.7 mm. of broad, flat ribbon inter- vening between the hinge plate and the echmidium. The crural proc- esses are given off just anterior to the hinge plate and are short, bluntly pointed projections of 0.1 to 0.2mm. The descending lamellae are about 0.5 mm. wide. The echmidium is broad and deeply cleft anteriorly, 1.9 mm. in a loop 4.6 mm. long. The junction or jugum between the descending lamellae is 0.62 mm. long in the above loop, or less in others, and is a narrow plate. The descending lamellae pos- teriorly face each other and their narrow edge is perpendicular to the inner surfaces of the valves. Anteriorly these ribbons turn about go° to become parallel with the inner valve surfaces and at the same time become fairly deeply concave and narrow distally. The hood rests on the inner ventrally curved edge of the descending lamellae. Anteriorly the hood is a widely flaring cone, expanded above but narrowing dor- sally. It also narrows posterodorsally with an opening half or less of the anterior dimensions. The base of the hood is continued posteriorly beyond its narrow termination as two converging septa which unite to form a low ridge at the proximal end of the echmidium (pl. 2, I, fig. 20). The posterior side of the hood varies from round to nearly flat and with its anterior deeply notched (pl. 1, I, fig. 26) or with only a slight trace of indentation (pl. 2, I, fig. 20). The notch is a variable feature which appears to be more prominent and more uni- form in smaller stages. Seen from the side the descending lamella forms a keel along the dorsal side of the loop, the base of the hood is deeply concave and the hood itself bulges prominently in a lateral direction. The ventral surfaces of the descending lamellae are convex and spinose, one set of spines on the outer edge and the other coming off the inner convex face. I2 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 A single specimen (U.S.N.M. No. 127205h) measuring 7.9 mm. in length and 8.3 mm. wide is unique in showing unequivocally the two descending branches free of each other (pl. 2, I, fig. 21). In this specimen the jugum has been resorbed because no evidence of break- age on the descending ribbons can be seen. This is the ultimate state in the development of the loop. Stages 8.1 to 9.0 mm.: A single specimen with loop (U.S.N.M. No. 127204e, not figured) representing these stages measures 8.6 mm. long by 8.4 mm. wide and is one of the largest specimens in the col- lection. The loop is 5.6 mm. long and the hood is 3.7 mm. long by 1.9 mm. wide. The hood is only moderately notched on the posterior side. The descending lamellae lie very close together but the jugum has been resorbed and the descending branches are free, the ultimate condition for the loop. If larger specimens exist it is likely that the only further change in the loop would be gradual lateral migration of the descending lamellae so that they would be more distantly spaced and subparallel. Median septum (or ridge): No distinct septum or median ridge was seen in specimens from I.0 mm. to 3.5 mm. After the latter length is attained a median ridge is discernible but even in large adults it is not a conspicuous feature of the shell. It is apparent that the ridge or septum never shared in the development of the loop as it does in so many modern long-looped brachiopods. Summary of loop development of Cryptacanthia.—The development of the loop in stages below 1 mm. can only be inferred from the early stage in the loop development of other brachiopods. In the earliest stages it is postulated that the loop originated as two processes grow- ing anteriorly from the hinge region, the descending branches de- veloping an angular bend medially and finally uniting distally at about the I mm. stage. The descending lamellae in these stages would be thin and delicate and no echmidium would have been formed (pre- centronelliform stage). After the 1 mm. stage the loop begins to thicken and at the place of junction of the distal ends of the descending lamellae the joined elements widen and flatten to form a plate having the shape of a spear- head and here called the echmidium (centronelliform stage). After the formation of the central echmidium the loop continues to strengthen, but at the anterior tip of the echmidium a bud appears in the form of a small elliptical cup. This is the incipient hood (early cryptacanthiform stage). In succeeding stages this structure expands and elongates with the growing loop. After the appearance of the hood the echmidium cleaves medially, the split lengthening and widen- 7 —_—<_<_¥_¥ NO. 3 LOOP DEVELOPMENT OF CRYPTACANTHIA—COOPER 13 ing with growth of the loop (cryptacanthiform stage). In the final stage of development the anterior cleft is completed and the descend- ing branches of the loop become freed of each other (early glosso- thyropsiform stage). THE LOOP OF CRYPTACANTHIA COMPACTA WHITE AND ST. JOHN Cryptacanthia compacta is the type species of the genus and for many years was the only known species. It is important therefore that the loop of the type species be clearly understood. As presently described and figured (Dunbar and Condra, 1932, pp. 307-309) the loop is depicted as a sort of cryptonelliform loop with long descending lamellae and long but fairly broad ascending elements. The figure of the loop given by Dunbar and Condra was reconstructed from serial sections. Study of the figured serial sections suggests that the ascending element is not properly restored and a new preparation of a loop inspired by this suspicion shows that it is entirely wrong. The new preparation of the loop was made on a specimen from Madison County, Iowa, essentially a topotype. The preparation was not made by the usual sectioning method although it was my inten- tion when I started the work to make serial sections. The first cut showed that the specimen was filled with clear calcite in two layers, an outer somewhat granular one and a solid inner layer of transparent light-brown calcite. On discovering this condition I scraped away the granular layer and part of the more solid mass beneath, washing fre- quently with acid to eliminate the needle marks. Soon a perfect loop was revealed which, however, was etched slightly too far on the dor- sal side. This too liberal etching removed the bulging part of the echmidium but left the jugum joining the descending lamellae. Study of the photographs makes it clear that these descending lamellae were joined like those from New Mexico. The preparation also reveals the numerous and long spines on the dorsal side of the descending lamellae which inspired White and St. John to name the genus Cryptacanthia. The specimen prepared was 5.3 mm. long and the loop measures exactly 4 mm. in length. On the dorsal side the descending lamellae are posteriorly distant but swing toward each other to be joined by a broad jugum 0.4 mm. long. Anteriorly from the jugum the de- scending lamellae are long and slender and diverge at a small angle. Their dorsal surface, from the posterior end of the jugum to the an- terior tip, is provided with long, slender, needle-like spines, the long- est one measuring 0.8 mm. in length. The descending lamellae an- terior to the jugum diverge at a low angle and curve strongly in an 14 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 anteroventral direction. At their distal end they bear an unusually large hood with very short attachment to the descending lamellae. The hood is greatly enlarged posteriorly where it measures 1.7 mm. in length but narrows to its base of attachment where it is only 0.5 mm. long. The hood is not attached posteriorly to the descending ele- ments. In ventral view the hood flares widely, 1.4 mm. wide, and the posterior edge is deeply notched. Comparison of the loop of C. compacta with that of C. prolifica— The loops of these two species are strikingly different. Posteriorly, that of C. compacta has more widely spaced descending lamellae and the jugum attaching these lamellae is longer and wider. The striking difference however is in the hoods. That of C. prolifica in the adult form has a long attachment and the posterior part is often extended as converging septa posteriorly along the inner edges of the descend- ing lamellae. The hood of C. compacta on the other hand is greatly expanded posteriorly and its attachment to the distal ends of the de- scending lamellae is very short. Only one loop of C. compacta was studied, but when this is compared with the many specimens of C. prolifica it seems evident that the loop of the Iowa species was pro- vided with more and longer spines than that of the New Mexico species. COMPARISON OF THE LOOP OF CRYPTACANTHIA WITH LOOPS OF OTHER PALEOZOIC GENERA The best-known long-looped Paleozoic brachiopod is Cryptonella whose loop typifies one major type of Paleozoic loop. It is like the end stage of both types of modern terebratellid loops. In Cryptonella the loop is simple in form and very slender in both ascending and descending elements. The development of this loop is not yet known but it is one of the most ancient of terebratulid loops as it occurs in the early Devonian. It is an odd fact that one of the most highly spe- cialized loops is actually one of the earliest. The loop of Cryptacanthia is not cryptonelliform although it simulates that loop in its late stages. The loop most like that of Cryptacanthia is that of Glossothyropsis. Although the loop of the type species of Glossothyropsis is yet un- known, other species have been taken from the Monos formation of Mexico and the Word formation of Texas which show well-preserved loops. The loop approaches the cryptonelliform loop in form, but the ascending elements are usually fairly broad and suggest the origin of the Glossothyropsis loop from that of Cryptacanthia. Elimination of the jugum joining the descending elements of Cryptacanthia and NO. 3 LOOP DEVELOPMENT OF CRYPTACANTHIA—COOPER I5 narrowing of the ascending elements will produce the loop of Glosso- thyropsis. The development of the external form of the two genera is also similar. Glossothyropsis is cryptacanthiform in its profiles and the disproportionate size of the two valves. The brachial valve of both genera is shallow. Glossothyropsis usually has a fairly strong median septum whereas that of Cryptacanthia is less well developed but far better developed than indicated by Girty. It is thus probable that Glossothyropsis is the ultimate stage of development of the cryp- tacanthiform loop. It is probable that the geologically youngest species of Glossothyropsis will be found with a loop advanced to the cryptonel- liform condition by narrowing of the ascending elements. COMPARISON OF THE LOOP STAGE OF CRYPTACANTHIA WITH LOOP STAGES OF OTHER TEREBRATULIDS The only known long-looped late Paleozoic brachiopods are Cryp- tacanthia, Glossothyropsis, Heterelasma, and an unnamed genus with cryptonelliform loop. The loop development of only the first one is now known. As described here Cryptacanthia passes first through a centronelliform stage (stages 1.5 to 3.5 mm.). The centronelliform stage characterizes a number of the earlier Paleozoic genera, such as Centronella, Nanothyris, Beachia, Oriskania, Rensselaeria and a few others (Cloud, 1942). No other adult loop is now known which represents the stages between 3.0 mm. and the point at which the jugum is completely absorbed. These stages of development of the hood are here called the cryptacanthiform loop. When the descending lamellae are free and the hood is represented by a broad ascending element with a broad transverse ribbon the loop is similar to that of Glossothyropsis and is called the glossothyropsiform stage. Comparison of these loop stages with the dallinid and terebratellid loops shows fundamental differences (Elliott, 1953). Both of the terebratellid families differ from Cryptacanthia in loop development in possessing a median septal pillar or septum in the initial stages. Cryp- tacanthia has only a modest median septum, and as revealed by C. prolifica this does not develop until the late stages of the ontogeny. Furthermore, the septum of Cryptacanthia is independent of the loop. In the terebratellids the median pillar is important because it is the site of development of the hood and median ring which produce the ascending elements of the adult loop. The loop-development stages of the Paleozoic Cryptacanthia thus bear little resemblance to the stages of development of the terebratel- lid genera even though the glossothyropsiform loop is similar to the 16 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 loop of Dallina or Magellania. The cryptonelliform loop, which con- sists of long, slender descending branches, slender ascending elements, and a slender transverse band, may be the ultimate stage in the de- velopment of the cryptacanthiform loop and is thus a parallel develop- ment of the ultimate terebratellid loop. REFERENCES Croup, P: E.,, Jr. 1942. Terebratuloid Brachiopoda of the Silurian and Devonian. Geol. Soc. Amer. Spec. Pap. 38, pp. i-xii, 1-182, pls. 1-26. Cooper, G. A. 1956. New Pennsylvanian brachiopods. Journ. Paleont., vol. 30, No. 3, pp. 512-530, pl. 61, fig. 1. (Issued in July.) Dungar, C. O., and Conpra, G. E. 1932. Brachiopoda of the Pennsylvanian system in Nebraska. Nebraska Geol. Surv., Bull. 5, 2d ser., pp. 1-377, pls. 1-44. Ex.iott, G. F. 1953. Brachial development and evolution in terebratelloid brachiopods. Biol. Rev., vol. 28, pp. 261-279. Wuitr, C. A., and Sr. Jonn, O. H. 1867. Descriptions of new Subcarboniferous and Coal Measures fossils col- lected upon the geological survey of Iowa; together with a notice of new generic characters observed in two species of brachiopods. Trans. Chicago Acad. Sci., vol. 1, pp. 115-127. EXPLANATION OF PLATES PLATE I Unless otherwise stated all specimens are from Grapevine Canyon locality. A. Cryptacanthia prolifica Cooper, new species. Figs. 1-3. Dorsal, ventral, and side views, respectively, of a complete loop, X 6, showing the rows of spines. From a specimen in the 7 to 9 mm. stage. Paratype U.S.N.M. No. 127205]. B. Glossothyropsis sp. Figs. 4, 5. Ventral and side views of the loop of a specimen from the Word formation, Glass Mountains, Tex., showing the narrow ascend- ing elements and the free descending branches, X 2. Figured specimen U.S.N.M. No. 127254. C. Cryptacanthia prolifica Cooper, new species. Fig. 6. Side view of a specimen 7.5 mm. long showing aberrant hood with cavity in its attachment to the descending branches, X 6. Para- type U.S.N.M. No. 127204n. D. Cryptacanthia prolifica Cooper, new species. Figs. 7-21. 7, View of the pedicle valve of the smallest specimen recog- nized as C. prolifica, X 8, paratype U.S.N.M. No. 127202j. 8-12, A series of 5 specimens showing juvenile forms with their open del- thyrium, X 4, paratypes U.S.N.M. Nos. 127205m-q, respectively. 13, View of the brachial valve of a complete specimen, 1, showing size ~ NO. 3 LOOP DEVELOPMENT OF CRYPTACANTHIA—COOPER 17 and form, paratype U.S.N.M. No. 127208z. 14, 15, Brachial views of two individuals more slender than normal, 3, paratypes U.S.N.M. Nos. 127208y and 127205s. 16-20, Anterior, posterior, side, pedicle, and brachial views, respectively, 3, of the holotype U.S.N.M. No. 127066. 21, Posterior half of a large adult showing the oval foramen and deltidial plates, X 6, paratype U.S.N.M. No. 127205t. E. Cryptacanthia prolifica Cooper, new species. Fig. 22. Posterior part of a brachial valve showing the cardinalia with the convex inner plate and its foramen, <.6, paratype U.S.N.M. No. 127205). F. Cryptacanthia prolifica Cooper, new species. Fig. 23. Imperfect loop, 6, with hood broken away to show the posterior extensions of the hood attachment and the jugum, paratype U.S.N.M. No. 127207p. G. Cryptacanthia prolifica Cooper, new species. Fig. 24. Partial side view of a small specimen, about 5 mm. long, show- ing small hood, spiny descending branches, and crural processes, X 6, paratype U.S.N.M. No. 127204s. H. Cryptacanthia compacta White and St. John. Fig. 25. Side view of a lump of calcite containing a complete loop, X Io, showing the small erect hood, hypotype U.S.N.M. No. 9382a. Speci- men from Pennsylvanian, Madison County, Iowa. Photograph taken under water. Note long spines in lower left. I. Cryptacanthia prolifica Cooper, new species. Figs. 26, 27. Posterior and ventral views, respectively, of a perfect loop showing the anterior notch in the hood, anterior cleft, and the crural processes, ca. X 10, paratype U.S.N.M. No. 127204t. (For additional views see pl. 2, G, figs. 13, 14.) PLATE 2 All figures of Cryptacanthia prolifica Cooper, new species, and all from Grapevine Canyon locality. A. Stage 1.6-2.0 mm. (precentronelliform stage?). Fig. 1. Early loop stage showing very slender and delicate loop, ca. X 15, paratype U.S.N.M. No. 127202k. B. Stages 2.1-2.5 mm. (centronelliform stage). Fig. 2. Specimen showing stouter descending branches than the pre- ceding which unite to form an echmidium, X 8, paratype U.S.N.M. No. 127206r. Fig. 3. Another brachial valve with well-preserved loop showing long, pointed echmidium, X 10, paratype U.S.N.M. No. 127202s. C. Stages 2.6-3.0 mm. (centronelliform stage or possibly early cryptacanthiform stage). Fig. 4. Brachial valve showing loop with echmidium and incipient bud (?) of the hood, X 10, paratype U.S.N.M. No. 127202u. Fig. 5. The loop of another specimen, 20, showing the elbow in the descending lamellae and the echmidium with a thickening, possibly the bud of the hood, paratype U.S.N.M. No. 127202w. 18 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 D. Stages 3.1-3.5 mm. (early cryptacanthiform stage). Fig. 6. Specimen with pedicle valve partially removed to show loop and the small hood seen from the ventral side, * 8, paratype U.S.N.M. No. 127206k. Fig. 7. Partial view from the dorsal side showing loop with small early hood, 8, paratype U.S.N.M. No. 1272033. Fig. 8. Another specimen showing trace of early hood, X 8, paratype U.S.N.M. No. 127203h. E. Stages 3.6-4.0 mm. (cryptacanthiform stage). Fig. 9. Specimen with part of brachial valve stripped off to show upper part of hood, X 8, paratype U.S.N.M. No. 1272031. F. Stages 4.1-4.5 mm. (cryptacanthiform stage). Figs. 10, 11. Side and partial side views of a specimen showing the small early hood and its slender attachment to the descending branches, X 8, paratype U.S.N.M. No. 127204h. Fig. 12. Side view of another specimen showing hood with long pos- terior extension, X 6, paratype U.S.N.M. No. 127204Cc. G. Stages 4.6-5.0 mm. (cryptacanthiform stage). Figs. 13, 14. Ventral and side views of an exceptionally well-preserved adult loop, 6, paratype U.S.N.M. No. 127204t. (For additional views of this specimen see pl. 1, I, figs. 26 and 27.) Fig. 15. Imperfect loop from dorsal side, 6, showing jugum, paratype U.S.N.M. No. 127203x. H. Stages 5.0-6.0 mm. (late cryptacanthiform stage). Fig. 16. Loop seen in side view and showing long attachment to de- scending branches and septumlike extensions posteriorly, < 6, paratype U.S.N.M. No. 127204q. Figs. 17, 18. Two anterior views of a specimen showing the expanded hood, <6, paratype U.S.N.M. No. 127204-0. I. Stages 7.1-9.0 mm. (late cryptacanthiform to early glossothyropsiform stages). Fig. 19. Adult loop seen from the laterodorsal view and showing the jugum, and the descending lamellae with their rows of spines, X 6, paratype U.S.N.M. No. 127204]. Fig. 20. Specimen seen from the posterior to show the posterior side of the hood, X 4, paratype U.S.N.M. No. 127205). Fig. 21. One of the largest specimens in the collection showing the de- scending lamellae from the dorsal side and absence of a jugum tying the branches together, < 6, paratype U.S.N.M. No. 127205h. ITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134, NO. 3, PL. 1 CRYPTACANTHIA PROLIFICA COOPER, NEW SPECIES, AND GLOSSOTHYROPSIS SP. (SEE EXPLANATION AT END OF TEXT.) VOL. 134, NO. 3, PL. 2) SMITHSONIAN MISCELLANEOUS COLLECTIONS | CRYPTACANTHIA PROLIFICA COOPER, NEW SPECIES | (SEE EXPLANATION AT END OF TEXT.) SMITHSONIAN MISCELLANEOUS COLLECTIONS VOLUME 134, NUMBER 4 Charles D. and Mlary Waux alcott Research Fund THE GEOLOGY AND VERTEBRATE PeLeEONTOLOGY OF UPPER.EOCENE STRATA IN THE NORTHEASTERN PART OF THE WIND RIVER BASIN, WYOMING PART 1. GEOLOGY (WirTH 1 Pirate) By HARRY A. TOURTELOT Geologist United States Geological Survey (PUBLICATION 4269) CITY OF WASHINGTON PUBLISHED BY THE SMITHSONIAN INSTITUTION MARCH 27, 1957 THE LORD BALTIMORE PRESS, INC. BALTIMORE, MD., U. S. A. CONTENTS TURES RO ERB eo eS OREIAIO OOS ir rc Era TERE mn ctie iets Oricon: ixestereal SEli YOb tHE ALECA jo. ded at Save v's: cc vlc wae ariidlale Otbe% wlais eRie'e's PUstoey Ol IVESPAMOI 0.85 se 6. oo Poi S lae ae dose vin keane ula iene es DREN LC CI PERETIES, 0 ak: ope ainiepnrquisisiate'ars Senha soin/mrasie «fables < tiga @elaiue)< SRM ss Area) Hae Oe x aos, se, laevie STS Sm teins we ere a araiaeiads MHGUNV IdaRIVEL LOLIMATOM «cvs alsvoucatee «file chute saelein gtelals a's sie erase Ree a ih eiee) Ptrail SORRIAIOM s fora iiss ssa) wisn odes wis wis Mere eles Nini) aya lavereieia Greenland brown member gc. c Osea kk asia oes sibs asides shie as aes Pfeuare Ianch MMegnWek’ e:cfe% civ cl pue pouress untpaw 07 pauterd auty St tmOT TPA BYSTT Aton Bursoyyeom umosq ystAvsd ‘auoyspues 2TueI[OA — 9 fakeyo pw paurei3 aury St auojspueg *uey aat[o Pue wer 02 UMOIG YSTKeIs ‘aucysde Oo SnoeIezzny puw auoyspuesS OTUEd[0A |---| Teuomepes9 aq 07 sueadde ene qoequco yeseq ‘aseq Jeou Ajie[rotqsed ‘sassew Je[ndaiit pue sasuey UT S1m90 azIsapuw FO SaTqqao pus satqqed papunos-[pam JO aqerdWO[D suo) ‘sassew AWt] Je[nJat1t pay ewos euTequCD ‘pauTe1Z asae0d 0} peurer3 aury ‘upard aatqo IYAtIq 07 UoAId pyereUB ‘aUOISaTTS ITUBITOA Aakeyo Aqayaty{s Ajuo !Aer8 ystmolpad ayIty Jutsayqeam AerZ ‘auoysa [ts Itued [oA —~ Aypoyq pue pasy st auojshey) ‘pauresd auty Alaa Sy BuO SPURS fueQ SATO AYTTT 09 UI Futsayjeam usesd ystAeid 03 wnolg ystdead ‘auoyske [> snosseyyny puB auO Spurs DTUPITOA 62-12 =t AvkeyT> ‘pauter9-wntpaw ‘ueei3 pyesewe ‘auojspues tue TOA, zjaenb [2 #T19p 200s suTeqUOO ptm ‘AsheTo ‘pautesd as.reoo 03 pautesd wntpaw ae ST !Aeld ysSwaoy[ad yIt] Ataa Butsayjeem ueq ‘auogspues 9 tuBdTOA —.}— — singoeifg Teproyouoos sey a pue prey st ‘herd aysty Aton Jutsayyeam Avid ‘auojsde[2 snoadeyyny, pOuuoTNOyY 9PKIHY uoljoes ysowUsaYyINOS ‘O63 “NOb 1 ‘22 208 Sms Zan adeyans pasaiyeam uo quepume ose ATpeooy syeashso aatuayag *Axem Yeynowlos pure AIT TS st ‘head ystuuea Jurrayiwam wnosrq ys thera yep ‘auoysAe po snosoeyyny, aoBsINs posayiBeM 247 UO aItuaTas Fo sTeySAI9 x pautoy -[ [IM puke aITUajaS snoIgty JO Sy@TUTEA SuTejuOD pu sINIeIF Teptopuoo e sey ay ‘paey pue ‘Axem ‘Aapts Apaystys st auoaske[D *suTeys UOIT UAOIq=US MOTTIA YITMH AesF qUsTT AeA 03 ssayIEOM fused @aTTO pue mO{[aA Fo satura yatm Aesd aysty] ‘auoysheTo snovoeyyny, aqytueyes autyyeysAio Ajyauty ynw sutequoo pue ‘Axem ywymauios ‘pipy ‘AIT IS ST auoysde [> heu9 ystuue [ [Mp Fursoyyeam umorq ystAerd yep ‘auoysde[o snosseyyny —. aqtuayas snoiqty Juepunqe sutequoo ‘Axem wa "QTATUOIUAG ‘UNOIG Ys THOT [AA IYTTT 09 MOTTA ‘oUcqshe TD SNOBIeF; NY sadoys pasayzeam yIOOWS UO QUEpUNqe ote STeISAIO aqTUaTaG “UOIT qt wsorq paureds AT[eooy AIT IS ATIYyITTS ‘head ‘ouoysAe Jo snovoeyznj —+ S| adoys susoy *Apues ATqyaty{s st AT[e20~ ‘Axem Qeymauios *Aayts ‘head ystuiorq yep 09 wAoIg YstAerd yep ‘auoysdv[> SNosdezyn] —- adoTs yi OoUs B SuOy pUe aInqoRIy Teptoyo suod apns e sey ‘Apues Ayaystys ‘paey ‘Ahake[d st auoqsa[ is *keag AYIIT Butsayywom pue moped pouteys Aj [eso] feig ‘9u0ysy[ ts ITUBDTOA, aoey [Bord stan Ayieau Suroy paq ysy ‘auoasde po Aypoyq Ai[ TS uMOIg-ystAesd JO SJSTSUOD PITY JOMOT ‘@[pptw JeoU Fynq OTIITA AedeTD pue Apues FO Peq IOO¥-¢ SNoNUTIUOSS TP YITA GUOISITIS Snoadezyny mOTToA-ys TAeId - FO Sqstsuoo spityy-omy aoddn ‘fauoqsayts pue auoyshe [2 snovoeyyny—+' aS Sie adpay sep ngori11 suroy C5 elec qtun frepnfaszt pue dieys st yoequoo yeseg “ea tSepue prey peutesd «381800 03 pauTvd-auTy Jo ple SPO DtozoaTeg Jo saTqqoo pw satqqead JO sassew Je[ndeary ase aseq qeay ‘*sayoqed Awry paey pue speq Kake yo Quwos suteqUOD pue paute1d-wntpew 07 pauterd-aury sx tsauoz uaesd ys the13 aWwos YITM UMOIG YSTMOT[AA 07 ABI YSTMOT[A ‘aUOISpLBS ITUBITOA— torr adoys suroy pue squewFesy Oryity Aww sutequoy ‘sassew AWTT] paey se[ndozrt yim agos pue ‘Aafs]o ‘pauresd asaeoo st ‘Surureqs uolt JO souoz pue syeaiqs sepnosir yy Aestd ystmo[[ed ‘auoqspues DTUedTOA—~}- 62 adoys swroy pte squauiery ItyIT] Auew sutequos tayos AakeTo ‘paureag-wntpow 03 poutesd-auty ‘Aead ystuaesd ‘auoqspues Otued [oA —— yaiou 03 SuTequnow wory paatiap $4201 otozoaTeg JO savatd Jo Furystsuod a#e ausdoysta[g Jo [2ae1d uewtpeg —- tS ©? +50 YINOS oF OE SIP FePNWY uoloeas ysowWwUsaYyJION NO. 4 GEOLOGY, WIND RIVER BASIN—TOURTELOT II member and are found in a fan-shaped area having its apex in a strike valley eroded in the Amsden formation of Pennsylvanian age on the north flank of the Owl Creek Mountains. The red color pre- sumably is derived from the Amsden formation, which contains red fine-grained rocks. Selenium-bearing vegetation on the green and brown member is detectable by its odor, particularly in the spring or after a shower of rain, in sec. 24, T. 40 N., R. go W., and at sev- eral places along the south flank of the Owl Creek Mountains in the northwestern part of T. 39 N., R. 91 W., and the northeastern part of T. 39 N., R. g2 W. The selenium content of the rocks is thought to be related to their volcanic constituents (Beath, Hagner, and Gil- bert, 1946). Uranium minerals have been found in the green and brown member at a few places (Love, 1954). Hendry Ranch member.—The green and brown member is over- _ lain by gray and greenish-gray claystone and siltstone and tan silt- stone rich in volcanic material in five areas along the northern mar- gin of the Wind River Basin. The easternmost, and largest, area lies between the Cedar Ridge fault and Badwater Creek in T. 39 N., Rs. 88 and 89 W., Natrona County. The other four are in Tps. 39 and 4o N., Rs. g2 and 93 W., Fremont County, in the western part of the map in figure 2. In each of these areas, the gray and greenish- gray unit and tan siltstone form the youngest part of the Eocene sec- tion. The new name “Hendry Ranch member” is applied to this se- quence. The name is derived from Hendry Ranch in the NE4SE} sec. 14, T. 39 N., R. 89 W., Natrona County, as shown on the topo- graphic map of the Badwater quadrangle. Good but discontinuous exposures of the Hendry Ranch member are found south of the ranch and to the southeast along Badwater Creek; from them was collected the largest part of the late Eocene fauna described by Gazin (1956) in Part 2. The type section (fig. 5) of the Hendry Ranch member is a composite one including three localities, all in Natrona County: locality 15 (fig. 2), NE4 sec. 31, T. 39 N., R. 88 W., which includes the contact of the Hendry Ranch member with the fresh-water lime- stone of the underlying green and brown member of the Tepee Trail formation ; locality 7 (fig. 2), SW4 sec. 14, T. 39 N., R. 89 W., which displays typical exposures of fossiliferous gray and greenish-gray rocks; and locality 16 (fig. 2), NE} sec. 23, T. 39 N., R. 89 W., which contains the tan siltstone that makes up the upper part of the Hendry Ranch member. The maximum preserved thickness of the Hendry Ranch member is about 550 feet, based on measurements in localities 7 and 16 above. 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Upper, locality 7 (see figs. 2 and 3), part of the type section of the Hendry Ranch member. Lower, locality 6, about half a mile east of locality 7. The ledge near the bottom of the sequence marks the same horizon at both localities. The first fossils from the Hendry Ranch member were found at these localities. (See table 1 for list of fossils.) = co I J \ i 5 ' : i i * a . —_ t — - > “. NO. 4 GEOLOGY, WIND RIVER BASIN—TOURTELOT 13 formation is made up of gray and greenish-gray andesitic volcanic sedimentary rocks and the upper part is tan volcanic siltstone. The greenish-gray unit has a maximum thickness of about 200 feet and the siltstone unit has a maximum thickness of about 350 feet. Single exposures of the lower unit do not reveal more than about 150 feet of strata. The siltstone unit is the youngest part of the sequence and its top is an erosional surface; the original thickness of the siltstone cannot be determined. The Hendry Ranch member is consistent in its major lithologic characteristics and is easily recognizable wherever seen, even in areas of only partial exposure. The member is confined to isolated areas of outcrop, and no facies changes were detected. The greenish-gray volcanic claystone and siltstone weathers to smooth badland slopes at most places. In general, the rocks in the greenish-gray unit are finer grained than the rocks in the underlying green and brown member. Irregular ledges of harder and more limy siltstone and sandstone are present in some exposures and one such ledge is particularly prominent at localities 6 and 7 (pl. 1). Thin beds of gray to black waxy claystone are present in the upper part of the same exposures. Crystals of selenite are abundant on the sur- face of most outcrops. Local lenses of fine-grained chert and quartz pebble conglomerate are interbedded with the tufts. The volcanic material in the rocks corresponds in composition to an andesite. The plagioclase feldspar is andesine, instead of labra- dorite as in the green and brown member of the Tepee Trail forma- tion. Not enough petrographic work has been done on the Tepee Trail to evaluate the significance of the apparent difference in feld- spars in the two members. Light-tan to greenish-brown biotite and hornblende are abundant and a few delicate shards of altered glass are present in most thin sections. At many places the rocks weather to a nodular surface very simi- lar to the “nodular zones” of the Oligocene sequences in Nebraska and South Dakota. Some of such nodular zones have been inter- preted as parts of paleosol complexes by Schultz, Tanner, and Harvey (1955). The nodular zones in the lower part of the Hendry Ranch member contain Glypterpes, cf. G. veternus, a large land snail, and also clay- and calcite-filled borings similar to the fossil larval cham- bers of insects described by Brown (1934, 1935), apparently indicat- ing subaerial conditions during deposition of the rocks. The nodules have yielded most of the fragmentary fossil vertebrates found in the Hendry Ranch member, a type of occurrence typical of the paleosol complexes reported by Schultz, Tanner, and Harvey (1955). 14 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 The tan volcanic siltstone unit of the Hendry Ranch member was found only along Badwater Creek north of Cedar Ridge and in a small area just north of locality 11 (sec. 10, T. 39 N., R. 92 W.). The siltstone is soft and forms poorly exposed slopes in contrast to the lower member, which forms badlands areas. The siltstone ranges in color from grayish tan to pale greenish gray, and gray; it is some- what limy throughout, poorly bedded, and irregularly jointed. At most places, two beds of white limy vitric tuff as much as 3 feet thick are present in the lower part of the sequence. The vitric tuff beds are highly lenticular and are missing at locality 16 (figs. 2 and 5). The siltstone unit contains much admixed volcanic material, however, particularly in its lower part. Lenses of bright-green volcanic-rich sandstone are present at some places. At locality 7 (figs. 2 and 5), medium-grained to coarse-grained volcanic sandstone at the base of the siltstone unit lies on greenish-gray claystone and siltstone. Lenses of conglomerate and coarse-grained sandstone made up of pieces of Pre-Cambrian and Cambrian rocks as much as I foot in diameter are common in the lower part of the siltstone unit and in the upper part of the greenish-gray unit. In some places, fragments of light-grayish-green siltstone from the lower unit are included in lenses of intraformational conglomerate in the lower part of the siltstone unit. The change from greenish-gray rocks below to tan siltstone above takes place within a few feet, but no consistent criteria were found for separating the two units along their contact. The most usable contact for field mapping is where the material in which the con- glomerate lenses are included changes from the gray claystone and siltstone of the lower unit to the tan siltstone of the upper unit. Where conglomerate or coarse-grained material is not present, this change occurs about at the base of a bed of white vitric tuff. How- ever, in local areas, there is prominent channeling at the contact. This channeling may account in part for the thinning of the underlying lower greenish-gray unit from place to place. The white clastic facies—The white clastic facies (fig. 3) con- sists chiefly of material eroded from the Owl Creek and Big Horn Mountains and deposited directly adjacent to the mountains or in reentrants within them. Volcanic material is mixed in different amounts with the derived clastics but the essential characteristic of the rocks of the white clastic facies is the general absence of volcanic material compared to the rest of the Tepee Trail formation, The white clastic facies is particularly well developed along the south side of the Owl Creek Mountains and is conspicuous in the area embraced NO. 4 GEOLOGY, WIND RIVER BASIN—TOURTELOT 15 by the forks of Dry Creek (Tps. 39 and 4o N., Rs. 92 and 93 W.). The facies is prominent also between the westernmost fork of Dry Creek and Hoodoo Creek. In the Dry Creek drainage, the facies consists of very light-gray to white pebbly and sandy claystone and very clayey sandstone. The rather uniform admixture of sand and pebbles gives the claystone a somewhat cementlike appearance. Al- though some of the sandstone beds show sorting and bedding, in general, the facies shows an absence of sorting during its deposi- tion. Pebbles of quartz and feldspar and abundant sand grains are scattered through the claystone like raisins in a pudding. The very poor sorting and general lack of bedding is suggestive of mudflows but no other evidence of this kind of deposition was recognized. Most of the clay beds in this sequence weather to a soft puffy surface and the clay in such beds probably is bentonitic. Some of the light-colored claystone is hard and only slightly plastic when wet. The forks of Dry Creek drain an area in the Owl Creek Mountains made up chiefly of pink to brown granite and the feldspars in these rocks could have yielded kaolinitic weathering products during Tepee Trail time. Such claystone may be kaolinitic but no mineralogical study was made. East of Hoodoo Creek, the facies is yellow to brown and contains several distinctive dull-red beds. Cobbles of granite and dark-colored gneiss, phyllite, and schist are abundant. The generally more som- ber color of these exposures and lack of the white claystone charac- teristic of the Dry Creek area is believed to be related to the dark- colored gneiss, schist, and phyllite in the area drained by Hoodoo Creek. The lateral gradation of the clastic material eroded from the mountains into the green and brown volcanic sediments of the Tepee Trail is well displayed along the sides of pediment benches in the area between Hoodoo Creek and the west fork of Dry Creek. The white clastic facies is typically developed along Lysite Creek (T. 40 N., R. go W.) and was derived chiefly from Paleozoic rocks. Red colors are common in the facies near where it overlaps Pennsyl- vanian and Permian rocks in the mountains. This is particularly no- ticeable in the reentrant in the Big Horn Mountain front in T. 39 N., R. 88 W., north of locality 1 (fig. 2). The equivalence of outcrops of the white clastic facies and the Hendry Ranch member of the Tepee Trail formation can only be inferred. The Hendry Ranch member is found only in areas isolated from the Tepee Trail strata adjacent to the mountains. At the same time, the equivalence of material of the white clastic facies and the Hendry Ranch member is believed certain because material of the white clastic facies is found in the mountains at altitudes much above 16 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 the outcrops of the Hendry Ranch member. Some part of the inter- mixed volcanic and clastic material in the Clear Creek Basin (fig. 6), for example, undoubtedly is equivalent to at least part of the Hendry Ranch member. Age.—The age of the Tepee Trail formation in the northeastern part of the Wind River Basin is considered to be middle(?) and late Eocene. The Hendry Ranch member has yielded a fauna that is late pT (Structure in pre-Tertiory rocks not shown) X5 exaggeration Cleor Creek lear Creek Badwoter Creek 2 | (Structure in pre-Tertiory rocks not shown) X5 exoggeration Fic. 6.—Cross sections along Clear Creek Valley (D’-D) and along ridge parallel to ae 1 mile northwest of Clear Creek (C’-C) showing Tepee Trail formation filling valley. Eocene in age and suggests equivalence with an upper Uintan stage according to Gazin (see Part 2). The green and brown member has not yielded many or very well preserved fossils but those that are known, according to Gazin, also are late Eocene in age. Locality lists of vertebrate and invertebrate fossils from the Tepee Trail forma- tion in the northeastern part of the Wind River Basin are shown in table 1. Tentative assignment of a possible middle Eocene age to the lower part of the Tepee Trail formation is based upon the absence of recognizable rock sequences yielding middle Eocene fossils in the northeastern part of the Wind River Basin and upon the relation of the Tepee Trail formation to underlying rocks in adjacent areas. The type Tepee Trail formation in the Absaroka Range lies uncon- formably upon the Aycross formation, the type area of which has yielded middle Eocene fossils (Love, 1939, p. 70). 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"9 uopoydonq ‘snasvg “yo snddiyidq youey Aipusyy ASMS ‘MO8-NOE-P1 coset Z ‘ds pstyg “ds sagsazqaj+) ‘snipaut “TJ ‘Jo snjnbo14 -04gaT ‘snunjoa] *q “y2 Uopoydopg “weayzj0u "(7 ‘JD Sdounqgojdiq ‘mossajag UOPOIsO}OA ‘Sisuazum * FT “yo Snposdok Fy “ds gsndopapidg youey AIpuszy ASUS “ANGG-NOE-P rs e Sisusbumokn snbpjouojt py “yaput yuspor “ds ounnpilpnjo1g ‘surqnp snanamas ‘prsurered Jajyews ‘prAuresed asiey “ds gstmpdvy ‘snudajaa2 * "Jo Sadgsajygajy “ds wnisayy -piad “ds guoposs0jdaT ‘snipam “yo snjnbpsjojdaT “wosaajag *q “‘taaavag uopoasojorg “ds gsnjkmarnjuag “ds gsndojgiayidy ‘snuny -03] "q "Jo uopoydonq “poo wmtsayjzoyoumsaq ‘syiav46 “yo sng GEOLOGY, WIND RIVER BASIN—TOURTELOT -Juyidq “ds guotsoumry ‘snjsngos "Py “yo Svp1py “yJapul e1oatuses) youey AspusyzyT MSMS ‘MG6Q-NOE-ET corte eG rds omy ‘wapkpy op ‘s1piqnjIags “7 "JO Siqaojpajsnp ‘synuis vapumnty ‘p1ausay Sispqowmosy Jle1y, veda yz, MNS ‘MS8S-N6E-ZE voceseee & 2'ds papumny ‘syiqnj2ads SIQAOIDAISN PY “WeI[IpOdOID “JapUl PIlIay}OWWOIG ‘snusapp uopoutmp [ery veday, ASMN ‘MS8-NOE-ZE sooree sre € 1 DINUAAD oby4a A ‘syiqnjoads siqaojoujsnp ‘sypwmosag *q °y9 og ‘sis -uasabprag *q “yo oskyg “ds vanumtT] ‘vjsnjaa “7 ‘sys vanumtT yre1y, veda zy, MSMS ‘MS88-NO6E-62 "oc" cer ce & ‘ds guopoukmp [ery veday ANMS ‘M8g-NOE-62 “cree S[Issoy Jequisur 10 uol}e00'T aequnu UOI}eULIO dey ote S a bumot yf “uispg daar puryy usajsvayjaou morl Sspssof auaz07q 4ag¢Q—t Alav], 18 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 the north face of Lysite Mountain, Tepee Trail strata lie with ap- parent conformity on lake beds of Green River type about 220 feet thick (Tourtelot, 1946). These lake beds are identical in type to those in the Tatman formation in the central part of the Big Horn Basin to the north. The relations between the Tatman formation and the lake beds and the overlying strata of the Tepee Trail formation of Lysite Mountain actually are indeterminable, but the available data suggest that middle Eocene time may well be represented in the lower part of the Tepee Trail. The top of the lake beds at Lysite Mountain is at an altitude of about 6,400 feet. On Tatman Mountain, 70 miles northwest of Lysite Mountain, the Tatman formation is about 700 feet thick (Van Houten, 1944, p. 194) and the uppermost beds preserved are at an altitude of about 6,200 feet. At Squaw Buttes, 55 miles northwest of Lysite Mountain, the Tatman formation is about 800 feet thick (Van Houten, 1944, p. 192), and the uppermost beds preserved are at an altitude of about 5,900 feet. Although the present altitude of the Tat- man formation is in part the result of post-Tatman structural move- ments (Van Houten, 1944), the essential uniformity of altitude of the youngest lake beds in the three areas mentioned makes it possible to interpret them as parts of a single episode of lake deposition. The Tatman formation is considered to be early Eocene in age in the central part of the Big Horn Basin (R. L. Hay, personal communica- tion, 1956), but the lake beds on Lysite Mountain could be either early or middle Eocene in age, or both. Even if the lake beds on Lysite Mountain should be considered to be middle Eocene in age, there is no line of evidence to suggest that all of middle Eocene time is represented there. The continuation of lake deposition from early to middle Eocene time in southwestern Wyoming and Utah is well known. Dane (1954) has shown that parts of the ancient Green River Lake persisted even into late Eocene time. Somewhat similar age relations of the lower part of the Tepee Trail formation can be deduced from the sequence in the Boysen area (Tourtelot and Thompson, 1948), just west of the area shown in figure 2. In the Boysen area, near Wind River Canyon, the Tepee Trail formation rests with apparent conformity on a brightly col- ored sequence continuous with the lower part of the Wind River formation. The brightly colored sequence was considered by Tour- telot and Thompson to be a part of the Wind River formation that might be of early middle Eocene age. This leaves most of the middle Eocene to be accounted for, and, provisionally, it is here considered to be represented in the lower part of the Tepee Trail formation of NO. 4 GEOLOGY, WIND RIVER BASIN—TOURTELOT 19 the northeastern part of the Wind River Basin. The Tepee Trail formation in the northeastern part of the Wind River Basin thus may include rocks of the same age as the upper part of the Aycross forma- tion in the northwestern part of the Wind River Basin. Van Houten (1950, 1954, 1955) has described a formation of both middle and late Eocene age, rich in volcanic material, along the south- ern margin of the Wind River Basin. This formation includes ma- terial from both the Absaroka volcanic center and the Rattlesnake Hills, a volcanic field of middle and late Eocene age in southern Natrona County. The middle Eocene part of this sequence is not separable from the late Eocene part of the sequence on a lithologic basis. STRUCTURE The Tepee Trail strata of the northeastern part of the Wind River Basin are moderately deformed. The most prominent structural fea- ture involving the Tepee Trail formation is the Cedar Ridge fault, which everywhere within the area of figure 2 forms the southern boundary of the Tepee Trail outcrop area. Most of the structural features within the outcrop area of the Tepee Trail are related to this fault, the displacement of which is indeterminable. A minimum displacement of about 1,000 feet, however, is indicated for that part of the fault in T. 39 N., R. 89 W. Here, a total of about 500 feet of Tepee Trail strata is exposed near the fault, and the top of these beds is about 500 feet below the top of Cedar Ridge which is made up of Wind River boulder beds. This is the largest displacement that can be demonstrated but the actual displacement on the fault may be much larger. In the Dry Creek drainage, the Cedar Ridge fault divides into several branches that enclose grabens in which Tepee Trail strata are found, and horsts made up of boulder beds assigned to the Wind River formation. Some parts of the faults in this area cut pre- Tertiary rocks. The Tepee Trail strata exposed along the north side of Cedar Ridge probably are cut by many normal faults of small displacement and extent. Only a few of these could be mapped and shown on figure 2. Most of the minor faults join the trace of the Cedar Ridge fault at large angles. Similar minor faults, essentially normal to the Cedar Ridge fault, probably cut Tepee Trail strata at other places along the Cedar Ridge fault but they could not be recognized. All are believed to be the result of adjustments in the relatively down- ward-moving block as the major faulting took place. 20 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 Near the mountains, the Tepee Trail strata dip at low angles away from the mountains. Some part of this angle of dip may represent original depositional slope; the rest is the result of the southward tilting of the mountain block in response to the movement on the Cedar Ridge fault. Near the Cedar Ridge fault, the strata dip north- ward at many places, the strata having been dragged upward by move- ment along the major fault. The age of the Cedar Ridge fault and associated structures cannot be placed more closely than post-late Eocene. It seems likely, how- ever, that the Cedar Ridge fault is as young as Pliocene, to conform with the pattern of normal faulting that resulted from epeirogenic uplift of the Rocky Mountain region, as pointed out by Love (1939, p. II4). SEDIMENTATIONAL HISTORY The sedimentational interpretation of the Eocene strata in the northeastern part of the Wind River Basin can contribute to the re- construction of the geologic history of the Wyoming basins, which has been reviewed by Van Houten (1952). This history, briefly stated, applies chiefly to the Wind River and Big Horn Basins and is one of mountain and basin formation in late Cretaceous and early Tertiary time, with the rising mountains shedding much debris into the basins by early Eocene time. Much of the present mountain topography had been shaped by the end of early Eocene time, which seems also to mark the end of differential movement between the mountain ranges and the basins until much later in Tertiary time. From middle Eocene time through at least some part of Miocene time, and perhaps into the Pliocene, the basins were progressively filled, chiefly with volcanic material from the Absaroka-Yellowstone volcanic region. As the basins were filled the mountain ranges were buried, and eventually a broad constructional plain resulted from which are inherited many of the features of the present drainage system. The process of basin filling was essentially continuous but it was interrupted locally from time to time (Love, 1952). During Paleo- cene and early Eocene time, the surfaces of deposition in the basins were not far above sea level, the increasing amount of sediments in the basins being accommodated by differential movements between the mountains and the basins. From middle Eocene time on, the surfaces of deposition were gradually raised higher and higher, in part because the sediments accumulated without basin sinking and perhaps in part because of progressive epeirogenic uplift. Epeiro- NO. 4 GEOLOGY, WIND RIVER BASIN—TOURTELOT 2I genic uplift had its major pulsation, or reached its culmination, prob- ably in Pliocene time, as pointed out by Love (1939). It is believed that faulting, represented by the Cedar Ridge fault, and others men- tioned by Love, by which the relations between mountain ranges and basins were again changed, took place at this time. The sedimentational history of Eocene rocks in the northeastern part of the Wind River Basin can now be discussed against this back- ground. The rocks of the Tepee Trail formation present two interest- ing sedimentational problems. One is the mode of transport of such large volumes of volcanic material. The other is the conditions that permitted the accumulation of volcanic material directly adjacent to a rugged topography in the pre-Tertiary rocks and prevented the ero- sion of them and the incorporation of the debris with the volcanic material. Discussion of these problems necessarily is speculative in large part. Perhaps a somewhat imaginative reconstruction of events and conditions will stimulate the gathering of data bearing on such problems. The Wind River formation in the northeastern part of the Wind River Basin represents a complex of depositional conditions. Ex- tremely coarse debris was shed by the mountains into the basin, as evidenced by the boulder conglomerate in Cedar Ridge and in the western part of the area included in figure 2. These conglomerate masses did not extend far into the basin, however, and at the time they were accumulating near the mountains red-banded fine-grained sediments were being deposited no more than 4 or 5 miles to the south. Apparently these were derived from the uplands, large areas of which were covered with red residual soil according to Van Houten (1948). The manner of deposition of the conglomerate has not been studied. The great size of some of the boulders suggests that mud- flows may have been important in moving the coarse material out of the mountains. Mudflow structures were not recognized in the con- glomerate, though, perhaps because they had been obscured by re- working of the mudflow masses by streams. In the Boysen area, west of that shown in figure 2, the mountain debris, none as coarse as that in the northeastern part of the Wind River Basin, was moved southeast from the mountain front by rela- tively short tributaries to a generally eastward-flowing master drain- age system (Tourtelot and Thompson, 1948). The locus of succes- sive levels of the master drainage system seems to lie about along the south margin of figure 2. The depositional pattern of the numerous channel sandstones that mark the locus of the drainageway does not 22 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 change as the eastern border of the Wind River Basin is approached, and it is concluded that the basin was open to the east during at least the later part of early Eocene time. Conditions of deposition of the Tepee Trail formation were quite different. First, the bulk of the sediment being deposited was derived from the volcanic centers in the Absaroka-Yellowstone region. Second, very little material was being eroded from the mountain ranges in contrast to the vast amount of debris that had been shed by them during early Eocene time. There is little or no evidence of any marked general climatic change, although the local climate prob- ably was somewhat modified by the seemingly great volcanic activity no more than 70 miles or so to the west. The well-developed bedding and rounded pebbles, cobbles, and grains of volcanic material indicate that the final agent acting on most of the material in the Tepee Trail formation was running water. Pond or quiet-water environments certainly existed, as is indicated by the fresh-water limestone and beds of claystone, but these seem to be minor in the environment as a whole. It is possible that the pebbles and cobbles of volcanic material were carried from their source to the northeastern part of the Wind River Basin entirely by streams. The presence of cobbles, however, seems to imply streams of great carrying power. Other evidence for such streams, such as channeling and relatively thick accumulations of conglomerate, are largely lacking. Also, it is difficult to imagine streams with such carrying power having courses essentially parallel to the mountain fronts and as close to them as the distribution of cobbles would indicate. At present, the volcanic breccia, tuff, and minor intrusive rocks of the Tepee Trail formation in the Absaroka Range form steep escarp- ments above the Wind River Basin on the south and the Big Horn Basin on the east. These erosional escarpments clearly have little relation to the possible former extent of the materials into the Wind River and Big Horn Basins. Squaw Buttes, in the southwestern part of the Big Horn Basin, is an isolated remnant of the Early Basic Breccia (Van Houten, 1944). Although the pieces of the rock have been somewhat rounded, and the mass should be called a volcanic con- glomerate (R. L. Hay, personal communication, 1956), the rock is similar in appearance and physical characteristics to the breccias of the Absaroka Range. Squaw Buttes thus appears to be a remnant of volcanic material in the deposition of which running water was not the dominant agent. Probably masses of volcanic material once ex- tended much farther into the Wind River and Big Horn Basins than NO. 4 GEOLOGY, WIND RIVER BASIN—TOURTELOT 23 they do now. Anderson (1933) has described volcanic mudflows that traveled much farther than the present distance between Squaw Buttes and the Absaroka Range, and on slopes that were similar to those that must have existed in the Big Horn Basin. The interpre- tation that formerly much more extensive volcanic mudflow masses were present in both the Wind River and Big Horn Basins is believed to be reasonable and helps explain the presence of volcanic cobbles in the northeastern part of the Wind River Basin. The volcanic cobbles have a somewhat peculiar distribution along the south side of the Big Horn Mountains. The northernmost sec- A’ A | Ttg j (Structure In pre-Tertiary rocks not shown) Sogebrush Draw Tig (Structure in pre~Tertiory rocks not shown) X5 exaggeration | Fic. 7.—Cross sections along Sagebrush Draw (B’-B) and along ridge parallel to |} and 1 mile west of Sagebrush Draw (A’-A) showing position of Tepee Trail forma- tion on north flank of Big Horn Mountains and in valley on south flank of mountains. tion of figure 4 illustrates this distribution. The rocks shown in the section are exposed at the mouth of Sagebrush Draw where that stream leaves a canyon as much as 500 feet deep in the pre-Tertiary rocks and has its course on the Tepee Trail formation. A cross sec- tion through this canyon and a parallel section through the ridge a mile west of the canyon is shown in figure 7. At the north end of the section, strata of the Tepee Trail formation from the main mass | of Lysite Mountain almost enter the upper part of the canyon. A remnant of Tepee Trail strata is preserved within the canyon, and Tepee Trail strata extend into the lower part of the canyon from its mouth. The strata in the northernmost section of figure 4 are very nearly within the mouth of the canyon, being less than half a mile distant from pre-Tertiary rocks both to the east and to the west. Vol- —— ee eee canic conglomerate is moderately abundant in a unit about 50 feet below the top of the Tepee Trail strata exposed there but, curiously, is present in somewhat larger amounts than similar-sized material ee 24 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 derived from the pre-Tertiary rocks. It is difficult to imagine how the volcanic material could have been placed almost within the canyon mouth by streams flowing eastward or northeastward in the Wind River Basin, even though a source for the volcanic material might have been a mudflow 50 or even 20 miles away. A similar topographic setting for Tepee Trail deposition is shown in figure 6, a cross sec- tion along Clear Creek, and a contrasting section along the ridge a mile west of the creek. In considering this anomalous distribution of volcanic conglom- erate, it should be recalled that both the Wind River Basin and the Big Horn Basin to the north were being filled at about the same time. Inasmuch as the Wind River Basin is believed to have been open to the east, and the Big Horn Basin was either closed or open to the north, there is no reason for the two basins to have filled at the same rate. Quite the contrary seems much more reasonable, in fact, when it is considered that volcanic material could enter the Wind River Basin chiefly through a relatively narrow passage at the northwest end of the basin. The middle and late Eocene volcanic material had ac- cess to the Big Horn Basin, obviously, all along the west side of the basin, 70 miles or so long. It seems logical to believe, therefore, that the Big Horn Basin was filled to the lowest topographic point be- tween the Owl Creek and Big Horn Mountains at a time when the floor of the Wind River Basin on the south side of the mountains was still several hundred feet below this point. The lowest point be- tween the ranges probably is concealed by the Tepee Trail strata along Bridger Creek (T. 41 N., R. 91 W.). As successively higher low points in the mountains were reached, such as the upper part of Sage- brush Draw, material would flood down the canyons to the south. Some downcutting of the canyons probably took place at this time and soon erosion into the Big Horn Basin fill permitted volcanic cobbles to move down the canyons and be deposited in their mouths. The white clastic facies of the Tepee Trail formation clearly repre- sents erosion of the mountains during Tepee Trail time. At very few places, however, do the rocks of the white clastic facies indicate as much vigorous sedimentational activity as suggested by the coarse volcanic sediments in the Tepee Trail. The general lack of sorting and possible mudflow deposition of some of the white clastic facies have been mentioned. The white kaolinitic appearance of some parts of the white clastic facies, particularly adjacent to areas underlain by granite, may be the result of leaching of iron from the early Eocene residual soils that were suggested by Van Houten (1948). Further investigation of this possibility would be interesting. a NO. 4 GEOLOGY, WIND RIVER BASIN—TOURTELOT 25 Although the white clastic facies and scattered fragments of pre- Tertiary rocks in the Tepee Trail formation, such as those at the mouth of Sagebrush Draw, indicate some erosion of the uplands of pre-Tertiary rocks, the amount of such materials seems anomalously small. This is particularly evident where the Tepee Trail formation was deposited at the foot of relatively steep canyons such as shown in figures 6 and 7. Whatever may have been the actual amount of material eroded from the pre-Tertiary rocks of the mountains in Tepee Trail time, it seems obvious that such locally derived material was considerably diluted and may have been masked by the larger amount of volcanic material. A further possible explanation related to the mode of transport of the volcanic material also seems attractive. Hypothetical mud- flows, of which possibly Squaw Buttes is the only remnant, have been suggested as an agent in the transport of cobbles of volcanic rock to the northeastern part of the Wind River Basin in addition to possible stream transport of such materials from the Absaroka source. Mud- flows of such magnitude seemingly would be most likely to occur during long-continued volcanic activity in the Absaroka-Yellowstone region. It is easy to believe that large amounts of relatively fine- grained ejecta would have been carried aerially to the east. The presence of glass shards in most rocks and abundant euhedral crystals of feldspar in some of the resedimented crystal tuffs point to such a condition. If this truly pyroclastic material was transported aerially to the northeastern part of the Wind River Basin and deposited on the slopes in large enough amounts, the streams would have been choked with such debris and incapable of eroding the pre-Tertiary rocks. The pyroclastic material would have moved down the slopes either by rill wash or various kinds of mass movement. The streams at the bottoms of the slopes were short, draining only the south sides of the Big Horn and Owl Creek Moutains, and their capacities would be overloaded by relatively small amounts of pyroclastic debris. Hence, except for canyons that may have been delivering material from the Big Horn Basin into the Wind River Basin, little pre- Tertiary material could be expected to be incorporated in the Tepee Trail formation even though it was deposited at the foot of well- developed highlands. The upper unit of the Hendry Ranch member reflects a rather large change in depositional conditions. Vitreous volcanic ash became really conspicuous for the first time in strata assigned to the Tepee Trail. In addition, erosion of the pre-Tertiary rocks seems to have become more effective, judging from the conglomerate made up of 26 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 Pre-Cambrian and Cambrian rocks in the lower part of the unit. Evi- dently, the rocks of later Paleozoic age now fringing the south side of the Big Horn Mountains for 3 or 4 miles both northwest and southeast of Clear Creek had been covered by older Tepee Trail strata, leaving only the Pre-Cambrian and Cambrian rocks of the highlands along the upper reaches of Clear Creek available for erosion. REFERENCES ANpeErsoN, C. A. 1933. The Tuscan formation of northern California, with a discussion con- cerning the origin of volcanic breccias. Univ. California Publ., Bull. Dept. Geol. Sci., vol. 23, pp. 215-276. BeatH, O. A.; Hacner, A. F.; and Grpert, C. S. 1946. Some rocks and soils of high selenium content. Geol. Surv. Wyoming Bull. 36, pp. 1-23. Brown, R. W. 1934. Celliforma spirifir, the fossil larval chambers of mining bees. Journ. Washington Acad. Sci., vol. 24, pp. 532-539. 1935. Further notes on fossil larval chambers of mining bees. Journ. Wash- ington Acad. Sci., vol. 25, pp. 526-528. Dang, C. H. 1954. Stratigraphy and facies relationships of upper part of Green River formation and lower part of Uinta formation in Duchesne, Uintah, and Wasatch Counties, Utah. Bull. Amer. Assoc. Petrol. Geol., vol. 36, pp. 402-425. Gazin, C. Lewis. 1956. The geology and vertebrate paleontology of upper Eocene strata in the northeastern part of the Wind River Basin, Wyoming. Part 2: The mammalian fauna of the Badwater area. Smithsonian Misc. Coll., vol. 131, No. 8, 35 pp., 1 fig., 3 pls. Hava eRe we. 1952. The terminology of fine-grained detrital volcanic rocks. Journ. Sedi- mentary Petrol., vol. 22, No. 2, pp. 119-120. Love, J. D. 1939. Geology along the southern margin of the Absaroka Range, Wyoming. Geol. Soc. Amer. Spec. Pap. No. 20, pp. 1-134. 1952. Preliminary report on the uranium deposits in the Pumpkin Buttes area, Powder River Basin, Wyoming. U. S. Geol. Surv. Circ. 176, Pp. I-37. 1954. Reconnaissance for uranium in the United States, Wyoming. U. S. Geol. Surv. Trace Elem. Invest. Rep. 440, issued by U. S. Atomic Energy Commission, Techn. Inf. Serv., Oak Ridge, Tenn., pp. 175-180. MaAsursky, HAROLD. 1952. Geology of the western Owl Creek Mountains (map). Guide Book, 7th Ann. Field Conf., Wyoming Geol. Assoc. Ossorn, H. F. 1929. The titanotheres of ancient Wyoming, Dakota, and Nebraska. U. S. Geol. Surv. Monogr. 55, vol. 2, pp. 1-953. NO. 4 GEOLOGY, WIND RIVER BASIN—TOURTELOT 27 ScHuLTz, C. B.; Tanner, L. G.; and Harvey, Cyrit. 1955. Paleosols of the Oligocene of Nebraska. Bull. Univ. Nebraska State Mus., vol. 4, No. I, pp. 1-15. Srncrair, S. J., and GRANGER, WALTER. 1911. Eocene and Oligocene of the Wind River and Big Horn Basins. Bull. Amer. Mus. Nat. Hist., vol. 30, art. 7, pp. 83-117. TourtTELoT, H. A. 1946. Tertiary stratigraphy in the northeastern part of the Wind River Basin, Wyoming. U. S. Geol. Surv. Oil and Gas Invest. Prelim. Chart 22. 1948. Tertiary rocks in the northeastern part of the Wind River Basin, Wyoming. Guide Book, 3rd Ann. Field Conf., Soc. Vert. Paleont., pp. 53-67. Also published in 1948 under same title in Guide Book 3rd Ann. Field Conf., Wyoming Geol. Assoc., pp. 112-124. 1953. Geology of the Badwater area, central Wyoming. U. S. Geol. Surv. Oil and Gas Invest., Map OM 124. Tourtetot, H. A., and THompson, R. M. 1948. Geology of the Boysen area, central Wyoming. U. S. Geol. Surv. Oil and Gas Invest. Map PM ot. Van Houten, F. B. 1944. Stratigraphy of the Willwood and Tatman formations in northwest- ern Wyoming. Bull. Geol. Soc. Amer., vol. 55, pp. 165-210. 1945. Review of latest Paleocene and early Eocene mammalian faunas. Journ. Paleont., vol. 19, pp. 421-461. 1948. Origin of red-banded early Cenozoic deposits in Rocky Mountain region. Bull. Amer. Assoc. Petrol. Geol., vol. 32, pp. 2083-2126. 1950. Geology of the western part of Beaver Divide area, Fremont County, Wyoming. U. S. Geol. Surv. Oil and Gas Invest. Map OM 113. 1952. Sedimentary record of Cenozoic orogenic and erosional events. Guide Book 7th Ann. Field Conf., Wyoming Geol. Assoc., pp. 74-79. 1954. Geology of the Long Creek-Beaver Divide area, Fremont County, Wyoming. U. S. Geol. Surv. Oil and Gas Invest. Map OM 1940. 1955. Volcanic-rich middle and upper Eocene sedimentary rocks northwest of Rattlesnake Hills, central Wyoming. U. S. Geol. Surv. Prof. Pap. 274-A, pp. I-14. WENTWorTH, C. K., and WiLLIAMs, HoweEL. 1932. The classification and terminology of the pyroclastic rocks. Nat. Res. Counc. Bull. 89, Rep. Comm. Sedimentation 1930-32, pp. 19-53. Woon, A. E. 1949. Small mammals from the uppermost Eocene (Duchesnean) near Bad- water, Wyoming. Journ. Paleont., vol. 23, No. 5, pp. 556-565. Woop, H. E., 2p.; Seton, HENRY; and Hares, C. J. 1936. New data on the Eocene of the Wind River Basin, Wyoming (ab- stract). Proc. Geol. Soc. Amer. 1935, pp. 394-395. Yen, TENG-CHIEN. 1948. Eocene fresh-water mollusca from Wyoming. Journ. Paleont., vol. 22, pp. 636-638. 1949. Corrections of fossil localities. Journ. Paleont., vol. 23, p. 320. 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Sa ave ce (6. fe 0.16 C18 O80 8 6 16 Une 86 penunucs—uoynjnbvo07 fo susayjog—l wavy 26 NO.6 HEMOLYMPH COAGULATION IN INSECTS——GREGOIRE 27 Homoptera.—Pattern I, with general solidification of the plasma, was consistently observed in Cicadidae, Cicadellidae and Fulgoridae. In the last family (Laternaria, Phrictus), coagulation of the hemo- lymph was especially substantial; the films of hemolymph were in- stantaneously transformed into opalescent bluish clots, embedding all the hemocytes (altered fragile hemocytes, numerous small macro- nucleocytes, and transitional forms to various types of granular hemo- cytes). Coleoptera—tThe various groups of Coleoptera listed in the table exhibited a great diversity in the reactions of their hemolymph in vitro. However, predominance of one of the patterns characterized several groups. Dark hyaline hemocytes, undergoing clarification after discharge of substance (see Heteroptera above, and Grégoire, 1955a, discussion, p. 129), were observed in Agra sp. (Carabidae) and in Veturius platyrrhinus (Passalidae). The reactions detected in Scarabaeidae (especially Melolonthinae, Rutelinae, Dynastinae) were essentially identical to those reported previously as representative of this family. Upon withdrawal, the hemolymph became immediately viscous and ropy. The hyaline hemocytes, relatively numerous (64 percent of the total hemogram in Lagochile sparsa Ohaus) and of small size, extruded spontaneously cytoplasmic expansions, soon embedded, like the other hemocytes, in the veil-like reaction developing in the plasma (pl. 1, fig. 6). In Zophobas latticollis Kraatz, pattern III, characterizing several species of Tenebrionidae, developed with a special clarity : cytoplasmic expansions of the hyaline hemocytes and transparent glassy veils (pattern II) appeared immediately upon withdrawal of the hemo- lymph. The consistency of the veils became granular, while circular areas of greater density (islands of coagulation: pattern 1) grew out around several hyaline hemocytes already involved in the constitu- tion of cytoplasmic systems (pl. 1, fig. 9). In the specimens of Sandalidae, the film of hemolymph consisted of a substantial syrupy granulum embedding tiny nuclei of altered unidentifiable hemocytes. The pattern of coagulation could not be safely established in these specimens. In Lampyridae, dense suspensions of particles normally present in the hemolymph of these insects, as in other groups (Coccinellidae, various Chrysomelidae), interfered with the detection of the pattern of coagulation. Among Cerambycidae, subfamily Prioninae (Stenodontes, Calli- 28 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 pogon) exhibited one of the most substantial coagulations recorded among all the insects examined in this and in the previous studies. Hymenoptera.—Rapid collection of the hemolymph without con- tamination with foreign tissues was difficult in small specimens and in dry ones. In ants, large numbers of specimens were used, and the only samples not discarded were those in which a limpid drop of hemolymph could be collected and a rapid spreading out of the films performed. In view of the scarcity of the species available and the large inter- specific and intraspecific variations in the reactions observed in this order of insects, the predominant patterns could not be established safely for several species and groups. Some patterns actually recorded in a part of the samples correspond possibly to incomplete reactions. Pattern I was observed in all the samples collected from all the females, males, and workers of Paraponera clavata (Formicidae) and Chlorion (Sphecidae), and pattern III in the three specimens of Mutillidae captured. In larvae of Camponotus sericeiventris, numerous hemocytes were loaded with refractile inclusions, and no modification of the plasma appeared in that material. The Hymenoptera listed in the table were characterized by the small size of their hemocytes and of the islands of coagulation around the hyaline hemocytes, even in the samples in which a substantial coagu- lation was recorded. In the latter preparations, a considerable ex- tension of the coagulation took place from around the islands of coagulation, which appeared in the granular clots as small circular areas of greater density, centered by the fragile hyaline hemocytes and remaining distinct in the general coagulation of the plasma (pl. 1, figs. 3, 4, 5). Lepidoptera (larvae).—In the two specimens of lepidopteran lar- vae, the reactions of the hemolymph in vitro were identical to those described and illustrated elsewhere in a large number of caterpillars (Grégoire, 1955, pp. 118-120 and pls. IX and X: pattern II, with large individual variations in the completion of the process, fre- quently incomplete, as in the two specimens listed in the table). In the films of hemolymph, refractile hyaline hemocytes underwent clarifi- cation after rupture of the cell boundaries and discharge of substance, as illustrated in figures 42-50 of the above-cited paper. DISCUSSION I. The four patterns used in the present study are an attempt to classify the disparities recorded in insects with regard to the micro- No. 6 HEMOLYMPH COAGULATION IN INSECTS—GREGOIRE 29 scopical picture of films of clotting hemolymph, observed by phase- contrast microscopy in standard conditions of preparation. Objection that these patterns might result from random artifacts has been examined elsewhere (Grégoire, 1955a). In control observations, the clotting process was compared in films of hemolymph spread out under glass by the standard procedure and in clot plugs spontaneously formed at the wound site and gently squeezed under glass after completion of the process. In both in- stances, the microscopical alterations characterizing the same pattern were recorded. The standard conditions of preparation of the samples of hemolymph seem therefore to be a faithful reproduction of the alterations occurring during the undisturbed natural process. 2. Whatever each pattern might signify at the cytological ? or bio- chemical level,* most results of the present and other studies * suggest 2 Among the factors implied in the process of coagulation, the patterns reflect actual inequalities between species and higher taxonomic groups in the degree of sensitiveness to contact with solid surfaces of the fragile hyaline hemocytes selectively involved in the inception of the coagulation, in the nature of the alterations undergone by these unstable cells, and in the rapidity with which these alterations develop. These differences affect the subsequent reaction of the plasma. As shown in the present and in previous studies, a similar degree in sensitiveness of the fragile hemocytes is frequently shared by insects belong- ing to a same group. A tentative identification of the fragile hyaline hemocytes has been reported elsewhere (Grégoire, 1953a; 1955a, p. 129). A part of these corpuscles exhibits cytological features in common with the oenocytoids. In several groups (Odo- nata, Hemiptera-Heteroptera, various species of Coleoptera, lepidopteran and dipteran larvae, Trichoptera, and some Hymenoptera) these corpuscles appeared in the films of hemolymph in the shape of highly refractive or dark hyaline hemocytes, which undergo clarification after explosive discharge of substance. The same corpuscles differ, however, in other characters from the classical description of the oenocytoids (1955a, discussion, p. 131). On the other hand, the fragile hemocytes selectively involved in coagulation are referred to by Jones (1954) as cystocytes, in Tenebrio molitor. 3 The scarcity of the data available at the present time does not enable one to establish whether actual biochemical differences characterize each of the four patterns, and especially the two aspects presented by the reactions in the plasma, the granular substance (in the islands of coagulation and in the areas of extension: pattern I), and transparent glassy veils (pattern II). As sug- gested by observations of films of varying thickness, it is unlikely, as reported elsewhere (Grégoire, 1955a, discussion, p. 128) that the twofold aspect of the plasma changes is related merely to differences in concentration or in thickness of the clotted films. The veils are not to be identified with the products of general disintegration of the hemocytes (cell fibrin). An adequate test of the validity of the patterns would be to determine whether biochemical differences correspond to microscopical pictures as dif- ferent as those consistently recorded, for instance, in insects belonging to the 30 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 that the patterns are not individual particularities, except in a few equivocal cases.’ The patterns rather characterize species, more fre- quently taxonomic groups (genera, families, suborders, or orders). Repeated samplings of hemolymph collected from several speci- mens of the same species, or from different species belonging to the same higher taxonomic category, made it possible to record consis- tently the same pattern in groups of various taxonomic importance such as the Orthopteroid complex (pattern I),* several families of Heteroptera (especially Reduviidae, Coreidae, Pentatomidae) (pat- tern IV), Belostomatidae and Nepidae (pattern 1), three families of Homoptera (Cicadidae, Fulgoridae, Cicadellidae) (pattern I), among Coleoptera, Hydrophilidae (pattern IV), Staphylinidae (pattern LVS several subfamilies of Scarabaeidae (Rutelinae, Melolonthinae, Dy- nastinae, Geotrupinae, Trichiinae and Cetoninae) (pattern II), Heteromera (Tenebrionidae, Lagriidae, Monommidae, Oedemeridae and Meloidae; patterns I and III), Cerambycidae (pattern I), Cur- culionidae (pattern IV), several families of Lepidoptera (larvae; pattern II), Tenthredinidae (patterns I and III). 3. Other groups (Cicindelidae, Carabidae, Dytiscidae, Silphidae, Passalidae, Coprinae, Elateridae) exhibited large intraspecific and interspecific variations in the patterns of coagulation recorded. In view of the diversity of the reactions in these groups, the pattern representative or predominant could not be established with certainty. However, at the genus level predominance of a pattern appeared in genera such as Carabus (pattern III), Agra (pattern 1), Hydaticus (pattern IV), Dytiscus (pattern III) Cybister (pattern 1), Necro- phorus (pattern I). 4. In the homogeneous groups listed above, the Neotropical ma- terial and the insects from the Old World supplied identical results orthopteroid complex (pattern I), in insects from several families of Scara- baeidae (Rutelinae, Melolonthinae, Dynastinae, Cetoninae) (pattern II), He- teromera (pattern III), and other groups of insects in which no visible modi- fication could be detected in the plasma (e.g., Staphylinidae, Hydrophilidae, and many Heteroptera) (pattern IV) under the phase-contrast microscope. 4Grégoire (1951, 1955); Grégoire and Jolivet (unpublished). The total material investigated consists of approximately 5,300 samples of hemolymph, collected from 3,400 specimens belonging to about 850 species. 5In most of these cases, the scarcity of the material available suggests that individual variations, incomplete reactions, or accidental artifacts (mechanical agencies; see Grégoire 1955a, p. 124ff.) might confuse the actual pattern. ®6In the highly homogeneous orthopteroid complex, differences in the inten- sity of the clotting reaction could be detected between several groups (see table). NO. 6 HEMOLYMPH COAGULATION IN INSECTS—GREGOIRE a5 with regard to the pattern of coagulation predominant or representa- tive of the taxonomic category. Such consistency suggests that the patterns of hemolymph coagu- lation are a character of taxonomic significance (in a broad sense). Whether that type of character is of more or less applicability in phylogenetical controversies, is a question left to competent phylo- geneticists. It might, however, be stressed that the process of hemo- lymph coagulation is in no way related directly to any type of struc- tural or ethological criteria commonly used for defining and grouping taxonomic categories. It is therefore of interest to check tentatively some taxonomic relationships on the basis of the presented data. 5. As pointed out elsewhere (Grégoire, 1955a, pp. 136-137), ran- dom coincidence does not seem to be entirely responsible for explain- ing some correlations between phylogenetic position of certain groups of insects and microscopical aspect of the coagulation of their hemo- lymph. In this respect, the Neotropical material examined here sup- ports former tentative suggestions concerning most of these corre- lations.” Pattern I has been heretofore uniformly recorded in Blattodea and in the other groups ranged within the orthopteroid complex. The mechanism involved in this pattern is identical to one of the types of coagulation described by Hardy (1892), Tait (1910, 1911), Tait and Gunn (1918), Numanoi (1938), and Grégoire (1955b) in crustacean blood, in which a special category of cells, the Hardy’s explosive cor- puscles, corresponding to the insect hyaline hemocytes or coagulo- cytes (Grégoire and Florkin, 1950), play a selective part in the in- ception of the coagulation of the plasma. Pattern I has also been recorded among various unrelated groups of insects, especially in groups characterized by the retention of various primitive characters, such as the Homoptera. In this respect, the present study has brought information on groups not represented in the material previously investigated. From these data, pattern I might be considered as a generalized primitive mechanism of coagulation of insect hemolymph. The mechanism of coagulation illustrated in pattern II has been observed, unmixed or predominant, in relatively recent groups of 7 After the completion of this paper, the patterns of coagulation were recorded in 400 insects collected in September 1956 at Tingo Maria (Peru) and in Octo- ber 1956 on Barro Colorado Island. The results are in agreement with those reported here, with regard to the predominance of one of the patterns in the following groups: Orthopteroid complex, Hemiptera, Homoptera, Scarabaeidae, Tenebrionidae, Cerambycidae, Curculionidae, Vespidae, and Diptera. 32 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 insects, such as Scarabaeidae (except Coprinae—see next paragraph) and lepidopteran larvae. As shown in the table, the present investi- gations have confirmed the predominance of the patterns previously reported for these groups. 6. In the samples of Neotropical species of Passalidae and of Coprinae, the islands of coagulation characterizing pattern I were absent or exceptionally recorded in the samples, while in the African specimens studied until now (Grégoire and jolivet, unpublished), these islands of coagulation appeared frequently or consistently in many samples. In view of the scarcity of the material and the diversity in the reactions characterizing these two groups, random variations might be responsible for these divergences between the results. SUMMARY Coagulation of the hemolymph in vitro has been investigated by phase-contrast microscopy in 630 specimens from 230 Neotropical species of insects. The present material includes samples of hemo- lymph from insects belonging to 17 families not represented in previ- ous related studies. A tentative classification of the process of coagulation into four patterns, suggested previously, has been used, and the patterns charac- terizing provisionally each species have been determined and reported in tabular form. The Neotropical material and the data collected formerly on species from the Old World (altogether approximately 850 species), sup- plied consistent results with regard to the predominance of some of the patterns in several taxonomic groups of various extension in the classification. In a condensed form, the investigations on the distribution of the patterns of hemolymph coagulation in the different orders have shown: (1) In the Orthopteroid Complex, a great uniformity of reaction, in the shape of pattern I, possibly a generalized primitive mechanism of coagulation of the hemolymph; (2) in several families of Heteroptera, absence of a visible reaction in plasma (pattern IV), in striking con- trast to two families of the same order, Belostomatidae and Nepidae, which exhibited a substantial coagulation (pattern I) ; (3) in Homop- tera, a substantial reaction in the shape of pattern I, representative or predominant, in Cicadidae, Fulgoridae, and Cicadellidae; (4) in Co- leoptera, as a taxonomic group, a large heterogeneity in the reactions. However, in this order, uniformity of reaction or predominance of a pattern was detected at the infraorder level, especially in Hydrophili- No. 6 HEMOLYMPH COAGULATION IN INSECTS—GREGOIRE 33 dae (pattern IV), Staphylinidae (pattern IV), Scarabaeidae (pattern II, with the exception of Coprinae: patterns I and III), Heteromera (patterns I and/or III), Cerambycidae (pattern I), Curculionidae (pattern IV), and in a few genera reported in the table; (5) in Lepi- doptera (larvae), predominance of pattern II, with the possible ex- ception of Saturniidae (pattern III); (6) in Hymenoptera, occur- rence of patterns I and III in several taxonomic groups, in Apidae, scarce coagulation or absence of plasma reaction. ACKNOWLEDGMENTS I am greatly indebted to James Zetek, former Resident Manager of the Canal Zone Biological Area, and Mrs. A. Gomez, secretary at the station, who did everything possible to facilitate my work dur- ing my stay at the laboratory on Barro Colorado Island. I acknowl- edge with sincere appreciation the assistance of Paul Swift, chief of the Eastman Kodak Tropical Research Laboratory, Panama City, who developed the photographic plates, and Messrs. Bocanegra and Ruiz who supplied me with several specimens. I wish to thank Dr. Remington Kellogg, Director of the United States National Museum and Dr. Waldo L. Schmitt, Head Curator of the Department of Zoology, for authorization to have the material determined in the Museum, and to express my gratitude to the fol- lowing for identification of the specimens: Dr. M. Beier, Dr. R. E. Blackwelder, O. L. Cartwright, Prof. L. Chopard, G. Fagel, Prof. W. D. Hincks, Ch. Jeuniaux, K. V. Krombein, M. N. Magis, C. F. W. Muesebeck, Miss S. Parfin, Miss L. Russell, Dr. R. I. Sailer, Dr. M. W. Sanderson, Dr. M. R. Smith, Dr. Thomas E. Snyder, T. J. Spilman, Geo. B. Vogt, Miss R. E. Warner, Dr. N. Weber, Dr. C. Willemse, Dr. W. W. Wirth, and Dr. D. A. Young. Special thanks are due O. L. Cartwright, Acting Curator of the Division of Insects, United States National Museum, for collecting and mailing the data; Dr. J. Leclercq for much information about taxonomic problems related to the present paper; and the Patrimoine de l’Université de Liége, for defraying the expenses of shipment of the microscope and equipment used in the present studies. 34 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 REFERENCES The literature on hemolymph coagulation in insects has been reviewed in the papers cited below under Grégoire, 1951, 1953a, and 1955a. Grécorre, CH. | 1951. Blood coagulation in arthropods. II. Phase contrast microscopic observations on hemolymph coagulation in sixty-one species of insects. Blood, vol. 6, pp. 1173-1108. 1953a. Coagulation de I’hémolymphe chez les insects hémiptéroides. Arch. Internat. Physiol., vol. 61, pp. 237-239. 1953b. Blood coagulation in arthropods. III. Reactions of insect hemolymph to coagulation inhibitors of vertebrate blood. Biol. Bull., vol. 104, PP. 372-393. 1953c. Sur la coagulation de I’hémolymphe des termites. Arch. Internat. Physiol., vol. 61, pp. 391-393. 1954. Sur la coagulation de I’hémolymphe des termites (deuxiéme note). Arch. Internat. Physiol., vol. 62, pp. 117-119. 1955a. Blood coagulation in arthropods. V. Studies on hemolymph coagu- lation in 420 species of insects. Arch. Biol., vol. 66, pp. 103-148. 1955b. Blood coagulation in arthropods. VI. A study by phase-contrast microscopy of blood reactions in vitro in Onychophora and in various groups of arthropods. Arch. Biol., vol. 66, pp. 489-508. Gr&GorrE, CH. AND FLorKIN, M. 1950. Blood coagulation in arthropods. I. The coagulation of insect blood, as studied with the phase contrast microscope. Physiol. Comp. et Oecol., vol. 2, pp. 126-139. Harpy, W. B. 1892. The blood corpuscles of the Crustacea, together with a suggestion as to the origin of the crustacean fibrin-ferment. Journ, Physiol., vol. 3, pp. 165-190. Jones, J. C. 1954. A study of mealworm hemocytes with phase contrast microscopy. Ann, Ent. Soc. Amer., vol. 47, pp. 308-315. NuMaAnol, H. 1938. On crustacean blood coagulation. Japan. Journ. Zool., vol. 7, pp. 613-641. Tarr: Ji. 1910. Crustacean blood coagulation as studied in the Arthrostraca. Quart. Journ. Exper. Physiol., vol. 3, pp. 1-20. 1911. Types of crustacean blood coagulation. Journ. Mar. Biol. Assoc., vol. 9, pp. 191-1098. Tait, J., and Gunn, J. D. 1918. The blood of Astacus fluviatilis: a study in crustacean blood, with special reference to coagulation and phagocytosis. Quart. Journ. Exper. Physiol., vol. 12, pp. 35-80. NO. 6 HEMOLYMPH COAGULATION IN INSECTS—GREGOIRE 35 EXPLANATION OF PLATE 1 Films of hemolymph spread out between slide and coverglass, immediately upon shedding from severed appendages. Phase-contrast microscope (Wild M/to). Scale: 20 microns. Figs. 1 and 2. Stenodontes (Mallodon) molarius Bates (Cerambycidae, Pri- oninae). (Pattern I***: very substantial coagulation.) All the hyaline hemocytes are surrounded by islands of coagulation. Considerable ex- tension of the granular coagulum. In figure 1, three elements belonging to other categories of hemocytes are passively embedded in the clot. Figs. 3, 4, 5. Paraponera clavata (Fabricius) (Formicidae). (Pattern I ***). Islands of coagulation of small size. Extension of the coagulum. In figure 3, a small hyaline hemocyte (on the right) in the center of a small island of coagulation. On the left, two granular corpuscles embedded in the clot. Fig. 6. Cetoninae sp. (Scarabaeidae). (Pattern II). Typical reaction of the hemolymph in vitro, as it appears in several subfamilies of this group (see table). Many hyaline hemocytes of small size with their cytoplasmic expansions are embedded in a substantial veil. Identical pictures were ob- served in several species listed in the table, especially in Lagochile, Pelid- nota, Phalangogonia, Trizogeniates, Aspidolea, Cyclocephala, and Dys- cinetus. Fig. 7. Phrictus quinquepartitus Distant (Homoptera, Fulgoridae). (Pattern [***), Two hyaline hemocytes, each surrounded by an island of coagula- tion. Considerable extension of the coagulum between the islands, which preserve their size and shape. Fig. 8. Pseudophyllidae (Tettigoniidae). Larva, first stage, male (Pattern I). The process of coagulation was slow and developed poorly in this specimen. When the picture was recorded, no reaction had yet developed in the plasma around the hyaline hemocyte shown in the center, between two other blood elements, including a granular hemocyte. Fig. 9. Tenebrionidae sp. Picture representative of pattern III, predominant in this family (see description of the coagulation in Zophobas latticollis Kraatz, in the text, p. 27). Fan-shaped disposition of the threadlike cyto- plasmic expansions of hyaline hemocytes, diverging from an air bubble on which these highly adhesive structures are anchored. Plasma reaction in the shape of a veil, with denser areas around hyaline hemocytes, correspond- ing to islands of coagulation. (Compare with Grégoire, 1055a, figs. II and 20. See legend of text figs. 2 and 3.) ‘ay thant di ‘a ks ee inane 000 ine Ry Tah wah ees me aay SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134, NO. 6, PL. 1 ae a , ee oth hts oe “be fi (See explanation at end of text.) SMITHSONIAN MISCELLANEOUS COLLECTIONS VOLUME 134, NUMBER 7 EARLY): WHITE, INFLUENCE UPON PLAINS INDIAN PAINTING GEORGE CATLIN AND CARL BODMER AMONG THE MANDAN, 1832-34 (WitH 12 PLaTEs) By JOHN C. EWERS Planning Officer for the Museum of History and Technology U. S. National Museum Smithsonian Institution ie ae SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134, NO° 7, -PEn 2 wg z at Hy ed Detail of Mandan robe showing style of painting a foot warrior. (Peabody Museum, Harvard University.) VO 1347 NOfd; RES 3 SMITHSONIAN MISCELLANEOUS COLLECTIONS (‘A}IstoAIUy) pleAreyy ‘IOLIINM poyuNoU Pv sulured jo ay Ays suwarcemson re ea ETS f aes EASY a : x ‘ winasnyy Apoqead ) SuIMOYs oqo1 uepuRryy fo Per VOL. 134, NO. 7, PL. 4 SMITHSONIAN MISCELLANEOUS COLLECTIONS ‘PE-cQr ‘uRpuRyY 94} SuoWe sysijIe 3} AA ‘porA\ NZ UPRITIWIXeyY 9UTIg sultAueduoooe (4Ystt ‘yresjtod-jjes) Joumpog Jie) ‘Zz “UTPJED IGAOI) “I _ ve, NO. 7 WHITE INFLUENCE ON INDIAN PAINTING—EWERS 3 rendered, elongated body which is geometric in character and drawn in outline only. The arms are lines extending outward from the shoulders and bent about midway of their length (i.e., at the elbows). At the ends of these arms are solid ball hands with the five fingers extended as lines. The legs are relatively short, bent at the knees. The grossly shaped upper legs are connected to linear lower legs. The foot is merely a continuation of the line of the lower leg at an angle from it. There is no attempt to portray body clothing. Yet the conventionalized representation of the phallus and scrotum may be an indication that the Mandan and their neighbors wore no breech- cloths at that period. Some contemporary descriptions of those In- dians also suggest the absence of the breechcloth in the men’s costume of the time. The enlargement of one of the mounted figures painted on this robe (pl. 3) shows the same style of rendering the head, arms, and body of the human figure. Notice that the man does not straddle the horse but merely sits atop it. There is no attempt to render the figure below the waist. The head and body of the horse are drawn in outline. The animal has neither eye nor mouth, but the ears are indicated one above the other and the mane is drawn in a conven- tionalized manner. The horse’s neck and body are decorated in geometric fashion with lines forming angular patterns some of which are partially filled with spots of color. As in the human figures, the upper legs of the horse are thick and the lower ones are mere lines. The hoofs are hook-shaped extensions of the legs. This primitive Mandan painting accented the general character- istics of the human form—the roundness of the head, the straight- ness of the limbs, the bilateral symmetry of the body, qualities Rudolf Arnheim has referred to as characteristics of the drawings of both primitives and children. (Arnheim, 1954, p. 131.) Details of the human figure were unimportant to the primitive Mandan artist. His head remained featureless. Bodies were crudely proportioned and appendages grossly generalized. Although his me- dium was paint, he used color sparingly. His heavy outlines gave to his work more the character of drawing than painting. He had no knowledge of color modeling or such other sophisticated concepts as foreshortening and perspective. When one object overlapped an- other he did not try to eliminate the outlines of the more distant one. Note the handling of the quiver carried by the warrior illustrated in plate 2. But generally there was no overlapping of human or animal figures which were scattered over the surface of the robe, each being rendered individually beside, above, or below the others. 4 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 Anthropologists customarily refer to this primitive work as picture writing, a term which aptly expresses the major motive for its crea- tion. The painter was more concerned with recording a memorable event by this pictorial shorthand than with the aesthetic appeal of his creation. He was more historian or biographer than artist. GEORGE CATLIN AMONG THE MANDAN, 1832 George Catlin (pl. 4, fig. 1), spent the summer of 1832 on the Upper Missouri. He traveled upriver on the first steamboat to ascend the Missouri to Fort Union, stopping briefly at Fort Clark, the American Fur Company’s post at the Mandan villages. He returned downstream by skiff, stopping over at Fort Clark for a period of two or more weeks. During that period the amazingly energetic Catlin created more than 4o pictures. Half this number were portraits of Mandan, Hidatsa, and Arikara Indians in the neighborhood of Fort Clark. The remainder were landscapes. Catlin was a self-taught artist whose forte was portraiture. He possessed a remarkable ability to catch a likeness of his sitter with a few swift, bold strokes of his pencil or brush. Catlin’s own account of his journey repeatedly referred to the Indians’ delight and amaze- ment at his ability to transfer their faces to canvas. They had seen nothing like this realistic portraiture before. (Catlin, 1841, vol. 1.) Catlin was less skilled in rendering the human body. His interest in the details of Indian costume and ornament usually was secondary to his keen desire to record faithfully the heads and faces of his subjects. Not infrequently, he exaggerated or omitted important details of dress. (Ewers, 1956, pp. 495-498). Nevertheless, Cat- lin’s very practice of painting from a model may have been a novelty in method of rendering the human figure that impressed some of his Indian sitters who had been familiar only with the generalized representations of humans created by native picture writers. CARL BODMER AMONG THE MANDAN, 1833-34 Carl Bodmer, on the other hand, was a meticulous draughtsman thoroughly trained in the best European traditions of drawing from the model. The German scientist Prince Maximilian zu Wied care- fully picked young, Swiss-born Bodmer (he was only in his early twenties) to accompany him on his travels in America for the pur- pose of making drawings that would illustrate his own scientific observations. The exacting scientist expected his artist’s record to be no less accurate in every detail than would be his own writings. VOM: 2347 NOs 7, RES SMITHSONIAN MISCELLANEOUS COLLECTIONS ‘VEQI * At aupog Aq pe AMMO Cnc ‘JsIj1B pue Jory puoooss uRpuRyY “STeog INO Tait © upped Aq }ietjIOg ‘I SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134, NO. 7, PL. 6 Detail of paintings on front of Four Bears’ shirt, collected by George Catlin in 1832. NO. 7 WHITE INFLUENCE ON INDIAN PAINTING—EWERS 5 The Prince and the artist ascended the Missouri on an American Fur Company steamer in 1833. (See Bodmer’s own field portraits of himself and the Prince, pl. 4, fig. 2.) They met some of the Mandan briefly on their way upriver in June. In the fall of that year, after more than a month of observation and picturemaking among the Blackfoot near Fort McKenzie, they returned to Fort Clark. There they spent the winter from November 8, 1833, to April 18, 1834, a period of more than five months. James Kipp, the fur company’s manager of Fort Clark, provided the German nobleman and his artist associate with a whitewashed room in a newly built wooden building within the fort which served them as living quarters, studio, and workroom. Throughout their stay, Bodmer worked as- siduously drawing and painting the likenesses of Mandan and other neighboring Indians in his studio, and scenes in the nearby Indian villages. He worked slowly and methodically, sometimes taking a full day or longer to complete a single portrait or view. During this period he created some of the most exact, realistic pictures of Ameri- can Indians ever executed. These pictures possess a remarkable sharpness and depth of focus. Not only are the faces of the Indians truthful likenesses, but the minute details of costume and ornament are precisely delineated. Although Catlin introduced realistic portraiture to the Mandan, the superior draughtsman, Carl Bodmer, showed them how every detail of a picture could be rendered with absolute truthfulness. Bodmer was the missionary par excellence of the white man’s tradi- tion of realism in art. Nor was Bodmer content merely to exhibit his own work among the Indians. He furnished some of them with paper and watercolors, and encouraged them to make pictures for him and for Prince Maxi- milian. In the collections belonging to the estate of Prince Maxi- milian zu Wied are no less than nine original Indian drawings on paper, collected during Maximilian and Bodmer’s trip to the Upper Missouri in 1833-34. THE CHANGING ART STYLE OF FOUR BEARS, MANDAN CHIEF Both Catlin and Prince Maximilian considered Four Bears the most remarkable man in the Mandan tribe. Although he held the rank of second chief, he was his people’s most popular leader. He was the son of a prominent warrior, Handsome Child. Four Bears himself, though of slight build and medium stature, claimed to have killed 5 enemy chiefs and to have taken 14 scalps. Upon his return 6 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 from a coup-counting session in the Mandan village of Ruhptare in January 1834, Four Bears told his white friends “with great satis- faction and self-complacency, that he had enumerated all his exploits, and that no one had been able to surpass him.” (Maximilian, 1906, vol. 24, p. 58.) Four Bears also was a leader in Mandan ceremonies. Prince Maxi- milian saw him lead a dance of the Dog Society, and learned that he had been selected as director of the great tribal religious festival, the Okipa, to be held the following summer (1834). Four Bears’ services to the traders and to visiting whites were many. Mr. Kipp relied upon him to protect the trading post at Fort Clark from the petty thievery of Mandan women and children. Maxi- milian found him to be his best authority on the language and religion of the Arikara, a tribe the scientist had no opportunity to visit. He observed that Four Bears spoke Arikara “fluently” (Maximilian, 1906, vol. 24, p. 73). The active, versatile Four Bears was also an artist. This hand- some, stout-hearted, friendly Mandan leader completely captivated George Catlin as did no other Indian among the more than 40 tribes Catlin visited. Catlin devoted a full chapter of his book to this warrior’s exploits and frequently referred to him elsewhere. He painted two portraits of Four Bears (his Mah-to-toh-pa), both of which are preserved in the collections of the U. S. National Museum (Nos. 386128 and 386131). One portrait shows Four Bears in mourning, bare to the waist, with scars on his breast, arms, and legs evidencing his past submission to the excruciating self-torture of the Okipa. The other (see pl. 5, fig. 1), painted in a day-long session, presents Four Bears at full length in his finest dress costume. Catlin collected this costume and displayed it for many years in his travel- ing exhibition. The handsomely quilled and painted shirt is pre- served in the U. S. National Museum (No. 386505). This shirt provides excellent examples of the art style Four Bears employed in depicting his war exploits in 1832 or earlier. On the right side of the shirt front he simply recorded his victims by painting their heads and upper bodies (pl. 6). On the back of the shirt he portrayed one of his coups (pl. 7). Note the very close similarity of this style to that of the painting on the buffalo robe collected by Lewis and Clark a quarter century earlier. Except for the crude representation of the features (two marks for eyes and one for the mouth), the rendering of the human figure is almost identical. It is definitely in the tradition of aboriginal Mandan picture writing. NO. 7 WHITE INFLUENCE ON INDIAN PAINTING—EWERS Z Shortly before Catlin left the Mandan, Four Bears invited him to a feast in his earth lodge and presented him with a robe bearing a representation of his most important coups. The chief had spent two weeks painting this robe during Catlin’s residence in the village. Unfortunately, the original of this robe is lost, and Catlin’s copy of the specimen, reproduced in his book and in one of his paintings in the American Museum of Natural History (pl. 8), appears to be an untrustworthy interpretation of the Indian artist’s style. Catlin adopted conventions of his own for rapidly rendering his copies of Indian pictographs. They appear to be more Catlin than Indian in style. Yet there is one detail in these paintings that Catlin surely did not invent—the hooklike hoofs of the horses, just like the horse hoofs portrayed by the unnamed Mandan artist prior to 1805. (See pl. 3.) Prince Maximilian and Bodmer came to know Four Bears (their Mato-Tope) even better than had Catlin. They first met him at Fort Clark in June 1833, on their way upriver, and the Prince bought from him “his painted buffalo dress,” suggesting that the clever In- dian was adept in dealing with white collectors. On their return to Fort Clark in November, Four Bears came to visit them in their studio. Prince Maximilian’s journal tells of his repeated visits to his quarters during their long stay at Fort Clark. Sometimes he spent the night on the floor before their fire. Four Bears exhibited an un- usual interest in Bodmer’s art. He brought other Indians to the studio to be painted and remained to watch the proceedings. He him- self posed for two portraits by the Swiss artist, one of which is re- produced as plate 5, figure 2. (The other, a full-length view in dress costume, is published as plate 46, in Maximilian’s Atlas). He also prevailed upon Bodmer to paint for him a white-headed eagle holding a bloody scalp in his claws. In return Four Bears painted for Maxi- milian a representation of his principal coups on a buffalo robe, and a separate rendering of one of his exploits, the conquest of a Cheyenne chief in hand-to-hand combat, apparently executed on paper. Although I have not been able to locate the originals of these works, they undoubtedly are reproduced with fidelity in Maximilian’s Atlas, plates 51 and 55. I include them here as plates 9 and Io. Comparison of the style of painting illustrated by the picture on plate 10 with that of the painting on Four Bears’ shirt (pls. 6 and 7), clearly reveals the great change in this Mandan artist’s style that took place during the period 1832-34. Gone were the knoblike heads, the stick figures, the crude proportions, the lack of detail. Heads were now painted in profile, the features sharply defined. Great care was taken in drawing a realistic human eye. The arms, legs, and 8 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 bodies were well proportioned, and the details of headgear, ornaments, and body costume, and the moccasined feet were delineated with painstaking care. Even though the colors of the original drawing are not known, some attempt at color modeling is suggested on the face and upper body of the warrior on the right. Can there be any doubt that this marked change in the painting style of Four Bears in the direction of a much more realistic treatment of the human figure should be attributed to the example of the white artists George Catlin and Carl Bodmer, whose artistic methods Four Bears had observed closely over a total period of several months? INFLUENCE UPON THE ART STYLE OF YELLOW FEATHER Next to Four Bears, the most frequent Mandan Indian visitor to Bodmer’s studio at Fort Clark during the winter of 1833-34 was a young warrior named Sih-Chida, The Yellow Feather. He was the son of a deceased Mandan head chief. Yellow Feather proudly showed Maximilian the Indians’ copy of the first treaty between his tribe and the United States, signed by his father and General Atkinson in the year 1825. Bodmer executed a full-length portrait of Yellow Feather in De- cember 1833 (plate 11, fig. 2, man on the left). Almost certainly this young man also posed for Catlin a year and a half earlier, although Catlin rendered his name “Seehk-hee-da, the Mouse- coloured Feather.” (See pl. 11, fig. 1.) Not only are the facial features of the Bodmer and Catlin portraits similar but the sitter wears a pair of long pendants of dentalia and large trade beads which appear to be identical. Maximilian wrote, “Sih-Chida, a tall, stout young man, the son of a celebrated chief now dead, was an Indian who might be de- pended on, who became one of our best friends and visited us almost daily. He was very polished in his manners, and possessed more delicacy of feeling than most of his countrymen. He never impor- tuned us by asking for anything; as soon as dinner was served he withdrew, though he was not rich, and did not even possess a horse. He came almost every evening, when his favorite employment was drawing, for which he had some talent, though his figures were no better than those drawn by our children.” (Maximilian, 1906, vol. 24, pp. 15-16.) Yellow Feather spent several nights in Maximilian’s quarters, sleeping on the ground before the fire. On one occasion he recovered Maximilian’s thermometer which he found concealed under the robe | SMITHSONIAN MISCELLANEOUS COLLECTIONS VO 1347 NOS eben Detail of paintings on back of Four Bears’ shirt, collected by George Catlin in 1832. VOL. 134, NO. 7, PL. 8 SMITHSONIAN MISCELLANEOUS COLLECTIONS ate et SFO Pre? Ss uIpe) owe NO. 7 WHITE INFLUENCE ON INDIAN PAINTING—EWERS 9 of a woman who had stolen it. On April 10, Yellow Feather left to join a large Hidatsa and Mandan war party against an enemy tribe. But sometime before his leavetaking, Yellow Feather painted at least two pictures in watercolors on paper for the Prince’s collection. One of these I here reproduce as plate 12, with the very kind permission of Karl Viktor Prince zu Wied. The style of painting the human and animal figures exhibited by this picture, though crude, is a far cry from the simple figures of traditional Mandan picture writing. The rider sits astride his horse rather than on top of it. His face is shown in profile and considerable emphasis is given to a realistic representation of the human eye. The eye of the horse, both the white and the ball, are shown with an equal concern for detail. The ears, nostril, and mouth are delineated. There is some grace in the entire horse figure. The hoofs are realistically formed in contrast to the hooklike conventionalized hoofs of traditional Mandan pic- tography. The figures have some degree of roundness achieved by elementary color modeling which is less apparent in the photographic reproduction than in the full-colored original. Although we have no earlier example of Yellow Feather’s art with which to compare this painting, I believe the influence of the white artists Catlin and Bodmer is reflected in this example of the effort of a young Mandan artist to portray details and to achieve realism in his figure painting. CONCLUSIONS The foregoing data provide perhaps the best documented case history of the influence of the European artistic tradition of realism upon the painting style of primitive American Indian artists of a century and a quarter ago. The details of this documentation are indeed remarkable. We know the characteristics of traditional Man- dan Indian picture writing as it was practiced prior to and at the time of these Indians’ introduction to the European art tradition. We know who the missionaries of the European tradition were (George Catlin and Carl Bodmer), and when they were active among the Mandan (1832-34). We know that these white men demonstrated the objectives and methods of realistic drawing and painting to the Mandan, and that they actively encouraged the efforts of native artists. We know who two of those artists were (Four Bears and Yellow Feather). We know that these Indians posed for both white artists a total of six times and that they watched the white men paint numerous portraits of other Indians. We have examples of the paint- ing of one native artist prior to the visits of Catlin and Bodmer, Io SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 and examples of the work of both artists, executed before Bodmer departed from Fort Clark, which clearly reveal the influence of European realism upon their painting styles. It is not possible or necessary to distinguish the separate influences of Catlin and Bodmer upon the work of these artists. Probably the cumulative effect of the examples and encouragement of two white artists, who visited the Mandan within a period of a little over a year, was important in impressing upon the native artists’ minds the possibilities of realistic representation of men and horses which found expression in their own later work. Significant, too, were the character and position of the two Indian artists who fell under the spell of the white artists’ realism. Both Four Bears and Yellow Feather were sons of prominent men in their tribe. They were not idle dreamers but active warriors, versatile, gregarious fellows. Certainly Four Bears was a decided extrovert, who numbered painting among his many interests and accomplish- ments. He was the antithesis of the American artist James A. McNeill Whistler’s conception of the primitive artist as a “man who took no joy in the ways of his brethren, who cared not for conquest, and fretted in the field—this designer of quaint patterns—this devisor of the beautiful—who perceived in Nature about curious curvings, as faces are seen in the fire—this dreamer apart, was the first artist.” (Whistler, 1916, p. 8.) Rather, the example of Four Bears would suggest that the artist in a primitive hunting culture was more apt to have been an active hunter and warrior, a fierce competitor, a wide-awake, keen participant in the affairs of his tribe, who enjoyed picturing the most exciting, heroic, and memorable of his rich experiences. There remains the problem of the relative permanence of Catlin’s and Bodmer’s influence upon Mandan Indian art. This is difficult to answer. Examples of Mandan painting in the late 1830’s and the 1840’s are lacking. Unfortunately, neither Four Bears nor Yellow Feather long survived Bodmer’s sojourn among the Mandan. Catlin claimed that ““Seehk-hee-da was killed by the Sioux, and scalped, two years after I painted his portrait.” (Catlin, 1848, p. 19.) The journal of Francois Chardon, who succeeded Kipp in charge of Fort Clark, repeatedly mentioned Four Bears’ activity as a warrior during the middle ’30s, but said nothing of his artistic endeavors. In the sum- mer of 1837 a disastrous smallpox epidemic decimated the Mandan tribe. Late in July of that year, Four Bears contracted that dread disease. He died a few days later. But before his death this courage- ous leader delivered a speech to his people denouncing the whites as VOL. 134, NO. 7, PL. 9 SMITHSONIAN MISCELLANEOUS COLLECTIONS (soppy Suerunxey) “9qo1 poyuted sivag Ino fo s[fuTsoRy s ToMpPod SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134, NO. 7, PL. - ear ~ - -_=a _~ Smt ita = - te _ £ v > — «. . a =~ ~ > : i Brows, on yy ., —— = 2 i * Facsimile of Four Bears’ painting of his victory over a Cheyenne chief. (Maximilian’s Atlas. ) pli; abit NO. 7, VOL. 134, SMITHSONIAN MISCELLANEOUS COLLECTIONS ( yy J] Je Joy}eIy MO]JOX ) ‘Taryd peasy uepueyy jo uos joryo pesy uepueyy | ‘€fQr ‘raupog Aq } (ed 1} Soa pue Jsqie ‘Toy}yea.t MOTI ‘ZEQT ‘ure Aq }eIVIOg “Ul SMITHSONIAN MISCELLANEOUS COLLECTIONS Wy hay Hynrr VOL. 134, NO. 7, PL. WWW T2O 12 watercolor by Yellow Feather. Original owned by the Estate of Prince Maximilian zu Wied. a Reproduction of NO. 7 WHITE INFLUENCE ON INDIAN PAINTING—EWERS II black-hearted dogs who had repaid his long and faithful friendship with a pestilence which was causing him to “die with my face rotten, that even the wolves will shrink with horror at seeing me.” Chardon wrote Four Bears’ brief obituary in his journal under the date Sunday, July 30, 1837: “One of our best friends of the Village (Four Bears), died today, regretted by all who knew him.” (Chardon, 1932, pp. 44-45, 50, 123-125.) BIBLIOGRAPHY ARNHEIM, RUDOLF. 1954. Art as perception. Berkeley, Calif. CATLIN, GEORGE. 1841. Letters and notes on the manners, customs, and condition of the North American Indians. 2 vols. London. 1848. A descriptive catalogue of Catlin’s Indian collection. London. CHARDON, FrANGoIS A. 1932. Chardon’s journal of Fort Clark, 1834-39. Ed. by Annie Heloise Abel. Pierre, S. Dak. Ewers, JoHN C. 1939. Plains Indian painting. Palo Alto, Calif. 1956. George Catlin, painter of Indians and the west. Ann. Rep. Smith- sonian Inst. for 1955. La VERENDRYE, PrerreE G. V. 1890. Journal of La Verendrye, 1738-39. Rep. Canadian Archives for 1880. Ottawa. Lewis, MERIWETHER, and CLARK, WILLIAM. 1906. Original journals of the Lewis and Clark Expedition. Ed. by Reuben Gold Thwaites. 8 vols. New York. MAXIMILIAN, ALEXANDER PHILIP, Prinz zU WIED-NEUWIED. 1906. Travels in the interior of North America. Jn Early Western Travels, ed. by Reuben Gold Thwaites, vols. 22-24. Cleveland. WHISTLER, JAMES A. McNEILL. 1916. Ten o’clock. Portland, Maine. yor ve 4 aia, Pr i ms ene hi : ae! 0%, cai A CREO i PATIL oy W ON pat wey sie eye a abel! NG HHA ai, be ua alain yal Pactiphiciiete: ‘ nit Sayan Pron an dak athiek dahl Rea eN My = a adh, var? Sigs dhl a Ah ol Ai Aa wi | SMITHSONIAN MISCELLANEOUS COLLECTIONS VOLUME 134, NUMBER 8 Charles D. and Mary Waux alcott Research Fund A SKULL OF THE BRIDGER MIDDLE EOCENE 'CREODONT,PATRIOFEEIS UETA VEIDY (WitTH 4 PLATEs) By C. LEWIS GAZIN Curator, Division of Vertebrate Paleontology United States National Museum Smithsonian Institution (PusiicaTion 4293) CITY OF WASHINGTON PUBLISHED BY THE SMITHSONIAN INSTITUTION APRIL 30, 1957 THE LORD BALTIMORE PRESS, INC. BALTIMORE, MD., U. S. A. Charles DB. and Mary Waux Walcott Research Fund A SKULL OF THE BRIDGER MIDDLE EOCENE CREODONT, PATRIOFELIS’ UETA’ LEIDY By C. LEWIS GAZIN Curator, Division of Vertebrate Paleontology United States National Museum Smithsonian Institution (WitH 4 PLatTEs) INTRODUCTION Discovery of a remarkably well preserved skull and lower jaws of the Bridgerian creodont carnivore Patriofelis was made by Golden York for the University of Utah. Not only is this by far the most nearly complete known for Patriofelis, but almost certainly belongs to the heretofore very poorly represented genotypic species, P. ulta. The specimen was found in 1953 while prospecting? Bridger exposures about 20-25 miles east of Kemmerer, Wyo., north of Granger and not far from the Green River. Mr. York’s description of the location would place it in or near T. 22 N., R. 111 W. The exact horizon is not certain but the specimen is reported to have come from near the top of the section as exposed locally in the hill or bench. The expos- ures in this general area are of the Bridger formation as shown on the 1955 edition of the Geologic Map of Wyoming. Moreover, there seems no doubt but that only the lower part of the Bridger is repre- sented in this portion of the basin. I am greatly indebted to Dr. William Lee Stokes, head of the de- partment of geology at the University of Utah, for giving me the opportunity of examining and describing this unusual specimen. Dr. Joseph T. Gregory at Yale University, Dr. Glenn L. Jepsen at Prince- ton University, and Dr. George G. Simpson at the American Museum of Natural History aided significantly in permitting examination and study of type and related materials in collections under their care. The specimen was skillfully prepared, removing it from the much- 1 Mr. York’s fieldwork was supported by a grant from the Research Fund of the University of Utah. SMITHSONIAN MISCELLANEOUS COLLECTIONS, VOL. 134, NO. 8 2 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 indurated nodule in which it was found, by Franklin L. Pearce. The wash drawings accompanying this paper were made by William D. Crockett. PREVIOUS STUDIES Matthew has briefly outlined the history of investigation relative to Patriofelis up to 1909. A recapitulation, however, with additional de- tails, and comments on more recent studies, may not be unwarranted. Patriofelis was first described by Leidy in 1870 from a pair of lower jaws (U.S.N.M. No. 105) collected by Hayden in 1869 near Fort Bridger. A major portion of both rami are represented, includ- ing alveoli for all the cheek teeth, but portions of the crowns of P,—M, are preserved only on the left side. Leidy did not so indi- cate, but it is evident from his illustrations of the right ramus pub- lished in 1873 (pl. 2, fig. 10) that the tooth portions shown were drawn in reverse from the opposite side. Leidy first regarded his new form, Patriofelis ulta, as probably belonging to the cat family, but in 1873 regarded it as “perhaps intermediate to the feline and canine animals.” In the meantime (1872) Marsh described the new genus, Limno- felis, with two new species, L. ferox and L. latidens, based essentially on a lower jaw portion with M, (Y.P.M. No. 11865) from Henry’s Fork and a last upper premolar (Y.P.M. No. 10904) from the Grizzly Buttes respectively. Later in the same year, with additional material at hand, he proposed the new generic name Oreocyon for Limnofelis latidens. Marsh did not discuss the possible relationships of these animals, other than to compare their size with that of a lion and to state that the lower canine and premolars of O. latidens “somewhat resemble those in the Hyaena.” He later concluded, however, that Limnofelis was apparently related to the cats, but nowhere did he discuss the possible relationship to Leidy’s Patriofelis from the same beds. Although rather generally ignoring Marsh’s names, Cope worked out a rather orderly arrangement of the creodonts and in 1880 (fig- ured in 1884a) described as new the form Protopsalis tigrinus on the basis of two lower molars (A.M.N.H. No. 4805), a canine and certain bone elements from the lower Eocene Wind River beds. He included this genus tentatively, as he had earlier allocated Patriofelis, in his family Oxyaenidae, which he regarded (1884a) as ancestral to the Felidae. The same year (1884b), however, he abandoned this idea in favor of the Miacidae as the ancestral group. In 1892, Wortman, in a part of a joint paper with Osborn on the no. 8 SKULL OF BRIDGER CREODONT—GAZIN 3 Wasatch and Wind River fauna, discussed and refigured the type of Patriofelis ulta and named as new the species ?Patriofelis leidyanus, based on a jaw portion in the Princeton collections (No. 11375) in- cluding, as was later shown, only deciduous teeth. Although uncer- tain as to the generic reference for his new species, he believed that it indicated for Patriofelis, along with Palaconictis, an ancestral posi- tion with respect to the true felids. Scott in his revision of the creodonts in 1892 also included Patriofelis in the Palaeonictidae, but placed Protopsalis along with Oxyaena in the Hyaenodontidae! He recognized, however, that Oreocyon Marsh, and hence that part of Limnofelis which had been named L. latidens, was a synonym of Patriofelis, but tentatively placed Limnofelis in synonymy with Pro- topsalis. Nevertheless, he followed Cope’s later thinking in deriving the Felidae as well as other modern Carnivora from the Miacidae. Wortman’s most significant contribution to the study of Patriofelis appeared in 1894 and included a detailed description of the mounted skeleton and other newly acquired materials in the American Mu- seum; He placed both Limnofelis and Protopsalis in synonymy with Patriofelis, concluded that only two species were represented, the large P. ferox and smaller P. ulta, and transferred the group to the Oxyaenidae. No reference was made to Marsh’s Oreocyon latidens ; presumably he regarded this as something different. Furthermore, the species that he had earlier named ?Patriofelis leidyanus was be- believed not to represent Patriofelis, but a form which might be the forerunner of the Nimravidae. Adams, in 1896, following Wortman’s suggestion, gave ?P. leidyanus the new generic name Aelurotherium, and because of it regarded the Felidae as polyphyletic. Wortman, in 1899, placed this genus in the Palaeonictidae, separate from the Oxyaenidae, and in 1gor placed his species A. leidyanum in synonymy with Marsh’s Limnofelis latidens as Aelurotherium latidens. This procedure, however, was in error as the immature lower jaw of Limnofelis latidens, with which comparison was made and which he figured as a type, was not the type but a referred specimen, and hence could not carry the name. The actual type of Limnofelis latidens, and hence of Oreocyon latidens, was a P* which Wortman in a later part of the same paper referred to Patriofelis ferox, clearly listing Lim- nofelis latidens as a synonym of Patriofelis ferox. Also in 1901 he described the new species Aelurotherium bicuspis on the basis of a lower cheek tooth, which he regarded as M, (Y.P.M. No. 11755). Although now recognizing that the known lower premolars of Aelu- rotherium were deciduous, he defended his 1892 conclusions as to the ancestral position of Aelurotherium with respect to the Oligocene 4 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 felids, resting them rather largely on his interpretation of M, as es- sentially the carnassial tooth of the lower series. Osborn (1907, fig. 95, E) reillustrated the teeth in the type of A. leidyanum indicating that all were deciduous and belonged to Patriofelis, but Matthew, in 1909, demonstrated the synonymous posi- tion of Aelurotherium, as well as Limnofelis, Oreocyon, and Pro- topsalis, with Patriofelis, correctly identifying the various teeth in the types. As to whether all the species that he placed in synonymy with P. ferox, however, represent that species and none P. ulta, may be doubted. In addition to describing the skeleton of Patriofelis ferox, Wort- man, in his 1894 paper, pointed out a number of characters that he believed indicated that Patriofelis or a closely related form gave rise to the pinnipeds. This suggestion was criticized by Osborn in 1900, and in 1902 Wortman defended his conclusion, taking a strong stand against Osborn’s views, but was again refuted, this time by Matthew in 1909. Kellogg, in 1922, discussed at length such evidence as had been presented on the origin of the pinnipeds, but deduced that a case for the Oxyaenidae had not been demonstrated, nor had Mat- thew’s suggestion of an arctoid fissiped ancestry solved the problem. Matthew’s (1909) monographic study of the Bridger carnivores and insectivores included a review and restudy of the known material of Patriofelis, as well as a taxonomic revision. The four species that he recognized are indicated as representing four distinct stratigraphic units and include as the oldest Patriofelis tigrinus (Cope) from the Wind River beds; a species from the Huerfano B beds originally re- ferred by Osborn (1897) to P. ulta, but named Patriofelis colora- densis by Matthew ; the genotypic species Patriofelis ulta Leidy from Bridger B; and Marsh’s Patriofelis ferox from the upper Bridger levels. In 1915 he decided that P. coloradensis represented Ambloc- tonus rather than Patriofelis. Later discussions of Patriofelis included a review by Thorpe (1923) in which an attempt was made to revive Patriofelis latidens. Thorpe recognized the error in Wortman’s taxonomic procedure in arriving at the name Aelurotherium latidens, but seems to have com- mitted a similar error in regarding the lower jaws, Y.P.M. No. 10940, as the type of Oreocyon latidens, whereas the holotype of Limnofelis latidens is No. 10904, a last upper premolar. Although Marsh’s char- acterization of the genus Oreocyon was based on referred materials, the type species was clearly that which he originally described as Limnofelis latidens and hence cannot have a different type specimen. In his revision of the ‘Pseudocreodi,” Denison (1938) revived no. 8 SKULL OF BRIDGER CREODONT—GAZIN 5 Protopsalis for the Wind River form P. tigrinus Cope because he felt that the carnassial construction exhibited had not attained the Patri- ofelis stage, and restored Huerfano B Ambloctonus coloradensis to Patriofelis, largely on the basis of characters of the lower jaw proper. A new species, Patriofelis compressa, was described, characterized by slender premolars, on a lower jaw (A.M.N.H. No. 17017) also from the Huerfano B stage in Colorado. P. M. Butler (1946) in a discussion of the evolution of carnassial dentitions in certain creodont subfamilies indicated the changes that took place in the development of the Oxyaeninae, culminating in Patriofelis. In his treatment of the various subfamilies he gave no preferred arrangement of these into families, but did discuss the general characteristics of the superfamilies or tribes as named by Matthew. TAXONOMIC SUMMARY The taxonomic arrangement adopted here is essentially that of Matthew, modified by Denison, but with minor differences and a cor- rected synonymy as far as known material can be interpreted. Al- though species are not redescribed, annotations are included where pertinent and a key is added. OXYAENIDAE Cope, 1877 OXYAENINAE Trouessart, 1885 PATRIOFELIS Leidy, 1870 Synonyms.—Limnofelis Marsh, 1872. Oreocyon Marsh, 1872. Protopsalis Cope, 1880. Aelurotherium Adams, 1896. Type.—Patriofelis ulta Leidy, 1870. Discussion.—The number of incisors above and below for the mid- dle Eocene or Bridger members of this genus is two in the material at hand, although Matthew has indicated (1909) that the number is three in the lower jaw, based partly on the appearance of alveoli in A.M. No. 12078. If Matthew has correctly interpreted No. 12078, the number of lower incisors in Patriofelis is variable as in Oxyaena. Moreover, Patriofelis has been characterized as lacking the second upper molar. Its presence, however, is variable, as a vestigial M? may occur, possibly characterizing lower Bridger P. ulta (and Huerfano species ?). 6 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 PATRIOFELIS ULTA Leidy, 1870 Synonyms.—Limmnofelis latidens Marsh, 1872; Oreocyon latidens (Marsh), 1872. Type——Lower jaws with P,—M, (incomplete) in left ramus (U.S.N.M. No. 105). Referred material—The upper premolar (P* according to Marsh, Wortman, and Thorpe, but P* according to Matthew) upon which Marsh based the species Limnofelis latidens is decidedly smaller than either P* or P* in A.M. No. 13145—the skull material described by Matthew as Patriofelis ferox. Its length is about intermediate be- tween that of P* and P* in the skull of P. ulta described in this paper. Moreover, this premolar is reported to be from the Grizzly Buttes and hence lower Bridger, the horizon which seems characterized by P. ulta. Hence, Limnofelis latidens and Oreocyon latidens are more likely synonyms of Patriofelis ulta rather than, as Wortman (1902) and Matthew (1909) indicate, of P. ferox. Besides the University of Utah skull and jaws (No. B50) belong- ing to Patriofelis ulta, there is in the U. S. National Museum (No. 21365) a right mandibular ramus of this species, with P,—P, par- tially erupted, Dp, loose, and M, and M, but little worn. The lower molars are only slightly smaller than in the type, but the horizon represented is believed to be very low in Bridger C, immediately above the Green River shale just to the northeast of Twin Buttes. PATRIOFELIS FEROX (Marsh), 1872 Synonyns.—Patriofelis leidyanus Wortman, 1892; Aelurotherium leidyanum (Wortman), see Adams 1896. Aelurotherium latidens Wortman (not Marsh), Igoi. Aelurotherium bicuspis Wortman, Igot. Patriofelis latidens Thorpe (not Marsh), 1923. Type-—Fragment of left ramus of mandible with M, (Y.P.M. No. 11865). Referred material—Included among the materials referred to Patriofelis ferox are the type specimens of the above species placed in synonymy. These are the immature lower jaw with Dp.—Dp, (P.U. No. 11375) of P. leidyanus ; the lower jaw with a canine, Dps, Dp,, and M (Y.P.M. No. 11756), which was “‘another specimen” in Marsh’s description of Limnofelis latidens, but which Wortman indi- cated as a type for Aelurotherium latidens; the lower cheek tooth regarded by Matthew Dp, (Y.P.M. No. 11755) of Aelurotherium bicuspis; and the symphysial portion of a pair of lower jaws with no. 8 SKULL OF BRIDGER CREODONT—GAZIN 7 C-P, (Y.P.M. No. 10940) which was among the “additional re- mains” Marsh had when he proposed Oreocyon for L. latidens, and which Thorpe regarded as the type of O. latidens when he attempted to preserve the species name Patriofelis latidens. Additional materials of Patriofelis ferox, including the mounted skeleton composed of A.M. Nos. 1507 and 1508 in the American Museum, are listed by Matthew (1909, p. 420). In the National Museum, besides the unused portions of A.M. No. 1508 (U.S.N.M. No. 5916) received in an early exchange, there are several parts of a comparatively large skull (U.S.N.M. No. 21364) obtained in the upper Bridger, probably C, to the north of the saddle between Sage Creek Mountain and Cedar Mountain, and the right ramus of a lower jaw, mentioned by Denison (p. 173) as exhibiting Dp.—-Dp, with M, erupting (U.S.N.M. No. 13318), from the upper part of Bridger C between Sage Creek and Hickey Mountain. M, in the latter speci- mens is not completely exposed, but its size is clearly much greater than in P. ulta. PATRIOFELIS (PROTOPSALIS) TIGRINUS (Cope), 1880 Type——Two lower molars, a lower canine, and certain bone ele- ments (A.M.N.H. No. 4805). Discussion—The type of this species is reported by Matthew (1915) to be from the Lost Cabin beds of the Wind River series. No additional specimens are known. I have retained Protopsalis as a subgenus rather than completely suppressing it in Patriofelis as Mat- thew did in 1909, and in preference to recognizing full generic rank as Denison did in 1938. Protopsalis appears to be structurally inter- mediate between O-xyaena and typical Patriofelis, but possibly a little closer to Patriofelis, although there is greater difference between it and Patriofelis than between the middle Eocene species of Patriofelis. This can perhaps be best represented by regarding it as a distinct sub- genus. Nevertheless, P. (Protopsalis) tigrinus is a rather gigantic form and surely is not the species which gave rise to the compara- tively small lower Bridgerian forms of Patriofelis. ?PATRIOFELIS COLORADENSIS Matthew, 1909 Type—Left ramus of mandible with C-P, and M, (A.M. No. 2691). Discussion.—I suspect, as did Denison (1938), that this species be- longs to Patriofelis rather than Ambloctonus where Matthew placed it in 1915. In addition to characters cited by Denison, I note that 8 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 Osborn’s (1900, fig. 8) illustration of the jaw shows the interval for missing M, smaller than would seem possible for this tooth in Ambloctonus. Moreover, Ambloctonus is not otherwise known from beds as late as Huerfano B or lower Bridger. PATRIOFELIS COMPRESSA Denison, 1938 Type.—Left ramus of mandible with C-M, (A.M. No. 17017). Discussion.—Slightly larger, though close to ?P. coloradensis in size, this form is apparently distinguished by relatively slender pre- molars. No information is available on the extent to which this char- acter is variable in Patriofelis. It comes, moreover, from the same beds as ?P. coloradensis. KEY TO SPECIES OF PATRIOFELIS M, with small talonid IMEGY MALE eee eicte cle SMa nG b wiclel s olelaoresideites P. (Protopsalis) tigrinus M, without talonid Taree PN. Gerted SEL) Se ccsles wiainn ace wees ls P. ferox Intermediate size (P,-M,, 75.5-76.0 mm.) * VGSU Tay les erie ae cite teers sie cies ones ne as ciess-<'e P. ulta Small Lower premolars robust (P,-M,, 60 mm.)*....?P. coloradensis Lower premolars slender (P,-M,, 65 mm.)*..... P. compressa * Measurements according to Denison, except second specimen of P. ulta. DESCRIPTION OF THE SKULL AND JAWS OF PATRIOFELIS ULTA Attention was called by Scott (1913) to the resemblance in relative body proportions of Patriofelis to an otter. The short, broad, and low snout of the skull is perhaps even more otterlike than he had realized. The general appearance of the skull was not hitherto known, as that of Patriofelis ferox which Wortman (1892) described (A.M. No. 1507) was considerably restored and the portions of the top of the skull were evidently placed too high, so that the rostrum has the appearance of much greater depth than in the University of Utah specimen. The latter shows a small amount of crushing dorsoventrally below the frontal region, but it is so nearly complete that the extent of deformation is evident and would in no way account for the depth - indicated in the larger animal. Dorsal aspect.—In dorsal view (pl. 1) the remarkable shortness and breadth of the rostral portion of the skull is clearly evident. The nasals are broad forward but taper posteriorly to near the fronto- maxillary sutures on either side where they abruptly widen and then no. 8 SKULL OF BRIDGER CREODONT—GAZIN 9 taper to a point between the frontals, producing a pattern resembling an arrowhead pointing posteriorward. The frontals are decidedly broad forward but taper posteriorly toward the parietals. Between the postorbital processes the frontal area or plateau is slightly con- cave, a condition that I do not attribute to the compression which has taken place between this surface and the posterior part of the palate. At the position of the postorbital processes the frontals are bluntly in- flated, and moderately prominent temporal ridges extend posteriorly to their union forming the sagittal crest at about the juncture of the frontal and coronal sutures. The parietals are elongate and slender, and support a moderately well developed sagittal crest that slopes downward and backward, although increasing in depth toward the supraoccipital. The supraoccipital is missing from the P. ulta skull, but from other material of the genus it is known to extend far back- ward and a little upward, forming a remarkably developed inion. The greatest constriction of the slender braincase is across the parietals between the temporal part of the frontals and the anterior margin of the squamosals where these pairs approach each other closest. Pos- terior to the constriction the superior and lateral surface of the cranium formed by the squamosal sweeps widely out onto the broad and massive zygomatic processes. At the deepest part of the temporal fossa, a very large vascular foramen penetrates the parietals on each side of the sagittal crest. This is accompanied by a smaller foramen posterolateral to it on each side close to the squamosal but also within the parietal. Lateral aspect.—In lateral view (pl. 2) the premaxilla is seen to rise aS a narrow rim of bone along the anterior margin of the maxilla and form the lateral rim of the broad but possibly somewhat de- pressed anterior narial aperature. The premaxilla is rapidly pinched out posteriorward between the nasal and maxilla. The maxilla as ex- posed laterally is anteroposteriorly short, although the nasal process extends posteriorly above the lachrymal as it rises onto the dorsal sur- face, and the malar process extends prominently backward beneath the malar or jugal. The large infraorbital foramen penetrates the maxilla above the anterior root of P%, well forward of the orbital rim and about midway dorsoventrally. The lachrymal bone is prominently displayed on the dorsolateral surface of the rostrum anterior to the orbital rim and forms the anterior margin of the orbit. Extending downward to the anterior extremity of the jugal and separated from it by a marked notch, it almost or quite excludes the maxilla from participation in the formation of the rim. The lachrymal foramen is concealed just within the orbital fossa posterior to a small process on 10 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 the lachrymal bone formed by the above notch. The jugal is compara- tively deep and strong, articulates in a much-extended contact with the maxilla below and inward, and shows almost no evidence of a postorbital process. Posteriorly, the squamosal portion of the zygoma is particularly deep and sturdy. The transversely elongate postglenoid process extends strongly downward and forward, forming with a prominent process on the outer part of the anterior margin of the glenoid fossa a combination which almost locks the condyle of the lower jaw in place. Unfortunately the mastoid and exoccipital por- tions of the skull are incomplete ; however, sufficient remains to note that the posterior profile of the occiput is nearly vertical beneath the inion. The orbits of Patriofelis ulta are not large but are decidedly dorsal in their position on the face. This is effected by the flattened to con- cave frontal area between them and by the deep zygomae below. Not only are the orbits high but the plane of the orbital rim faces decidedly upward because of the outward sweep of the jugal. The anterior margin of the orbit is well forward, about over the middle or anterior portion of P*. It is only in the orbital fossa that there is any evidence of dorsoven- tral compression of the skull; nevertheless, the noticeable fracturing and distortion are not so severe that details of the foramina penetrat- ing bone in this area cannot be determined, although certain of the sutures are obscured. The large posterior opening of the infraorbital canal is just below and slightly median to the lachrymal foramen, at the anterior apex of the orbital plate of the maxilla. Posterior to the infraorbital opening, a little over 2 centimeters, and about on the same level, there is a large, anteroposteriorly elongate sphenopalatine foramen, and immediately below the latter is a much smaller, though prominent, posterior palatine foramen. In the posterior portion of the orbital fossa, a separate optic fora- men seems indicated by an opening about 14 centimeters anterior and dorsal to the sphenoidal fissure. The large sphenoidal fissure, directly below the most constricted portion of the cranium, evidently trans- mitted not only the third, fourth, first branch of the fifth, and sixth cranial nerves as customary, but also the second branch of the fifth or trigeminal, inasmuch as the foramen rotundum does not appear to have become separated from the sphenoidal fissure (Wortman be- lieved them separate), at least not externally, in this group of animals. Moreover, the sphenoidal fissure must also have transmitted the ex- ternal carotid artery, as the anterior opening of the alisphenoid canal, which, when present as in modern bears and dogs, opens into the No. 8 SKULL OF BRIDGER CREODONT—GAZIN II foramen rotundum, was evidently confluent anteriorly with the sphe- noidal fissure. The posterior opening of the alisphenoid canal is surely represented by the clearly defined foramen immediately anterior to the foramen ovale (agreeing here with Wortman’s interpretation). Ventral aspect——In the over-all appearance of the skull in ventral view (pl. 3), one notes the short, broad palate, elongate mesoptery- goid and basicranial portion, and widely swinging, massive zygomae. The palate in greater detail shows the premaxillae not much extended forward of the canines and nearly straight across the front of the incisors. The anterior palatine foramina are close to the incisors and median to the canines. They appear nearly circular when viewed from somewhat forward of the palate. The posterior palatine foramina are on the forward portion of the suture between the maxillae and palatines, medial to the fourth premolars. The posterior nares are cov- ered beneath by the palate to a point farther back than the posterior border of the orbital plate of the maxilla on either side, about medial to the posterior margin of the carnassials. The mesopterygoid fossa is extremely elongate anteroposteriorly and the forward portion is partially constricted below by inwardly directed lower margin of the ascending plate of the palatines. Posteriorly the fossa is more open as the pterygoids along their lower margins diverge toward the hamu- lar processes. The posterior margin of the pterygoids, above the hamular process, sweeps abruptly upward and posterolaterally just inward of the foramen ovale, apparently extending almost to the notch representing the foramen lacerum medius. Particularly noteworthy is the union of the pterygoids across the roof of the mesopterygoid fossa, concealing the presphenoid and the anterior portion of the inferior surface of the basisphenoid. Anterior to this the evidence is not so clear, but there seems no doubt but that the palatines are also united through a median suture completely removing the presphenoid from participation in the mesopterygoid fossa, not, however, the vomer, the median ridge of which can be seen emerging from the nasal cavity. In the basicranial area only the basisphenoid, basioccipital, and periotics are preserved posteromedial to the squamosals and alisphe- noids. The basioccipital is broad as well as elongate, evidently occu- pying a relatively large area of the basicranial region. The basilar tubercles for the recti capitis muscles on the forward portion of this bone are elongate and well developed, reaching their greatest promi- nence forward at the suture between the basioccipital and basisphe- noid. Posterolaterally, the basioccipital is perforated by a broad and flattened condylar or hypoglossal foramen which joins a prominent I2 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 vascular canal before entering the foramen magnum. Medial to the hypoglossal foramen and extending ahead to the lateral margin of the basioccipital, a broad and distinct anterolaterally directed groove, evidently occupied by the internal carotid, as suggested by both Wort- man and Matthew, rises into the large aperture representing the fora- men lacerum medius just ahead of the medial portion of the petrosal. The exposed surface of the basisphenoid is triangular in shape with the anterolateral sides bound in part by the alisphenoids and forward by the V-shaped margin of the pterygoids. About midway forward on the anterolateral margin on each side, at the anterior extremity of a shallow groove from the foramen lacerum medius, there is a fora- men which extends forward above the pterygoid, eidently the ptery- goid canal for the Vidian nerve. Parallel and lateral to this on the surface of the alisphenoid are two or three sharp grooves or striae, extending between the posterior margin or lip of the foramen ovale to the position on the margin of the aperture corresponding to the eustachian foramen. Still more lateral and nearly parallel to the fore- going, but on the squamosal, is the straight and deeply impressed fissura Glaseri, for the chorda tympani nerve, sharply limiting the glenoid surface and postglenoid process medially and extending back- ward to a recess in the squamosal directly opposite the fenestra ovalis. The posterior surface of the postglenoid process shows a number of dorsoventral ridges and grooves near the lower margin, and a very broad and shallow depression near its medial margin extends upward and is confluent with a comparatively large postglenoid foramen (Wortman thought this to be absent) close to the fissura Glaseri. Petrosal.—The petrous portion of the periotic is exhibited in the anterolateral portion of the large otic fossa lateral to basioccipital. It does not appear to separate completely the foramen lacerum medius from the foramen lacerum posterius as the medial margin of the petrosal shown on the left side approaches close but does not touch the basioccipital. The outline of the petrosal as exposed ventrally can- not be fully determined because the margin is somewhat damaged and incomplete ; nevertheless the most conspicuous feature of this ele- ment is the downward- and forward-directed buttonlike promontorium. A fairly large fenestra rotunda faces backward and slightly outward. An elongate groove on the petrosal extending backward from a posi- tion immediately outward from the lateral margin of the fenestra rotunda is not explained but suggestion is made that this may have covered the stapedial muscle dorsally, or possibly the stapedial artery. The slightly smaller fenestra ovalis is forward and a little above the fenestra rotunda and faces laterally and somewhat forward. no. 8 SKULL OF BRIDGER CREODONT—GAZIN 13 The ventral aperture of the stylomastoid foramen is destroyed on both sides but sufficient remains of the walls of the foramen to indi- cate that it may not have been completely closed medially. A small portion of the mastoid projects medially, in front of the stylomastoid foramen and beneath its continuation as the facial canal, almost to the petrosal posterolateral to the fenestra rotunda. Immeditely lateral to the stylomastoid foramen and confluent with it, as exposed in the broken section, is a larger cavity (or canal?) that may have contained the stylohyal. The facial canal is open anteriorly at least as far as a point just ahead of the fenestra ovalis. Here the facial nerve may have entered the petrosal, although slight damage obscures the rela- tionship. On the other hand, a large aperture on the dorsal surface of the petrosal, posteromedial to the promontorium, may have con- ducted the facial nerve, in which case it was uncovered ventrally through most of its course. The large aperture referred to is not otherwise accounted for. A prominent epitympanic recess is noted, ap- parently in the squamosal, opposite the fenestra ovalis and at the posterior extremity of the fissura Glaseri. Upper dentition—In a superficial way the teeth (pl. 3) of Patri- ofelis, as noted by Marsh, show an interesting resemblance to those of the hyena. Although the form of the palate is rather like that in Crocuta, the pattern of the upper teeth is perhaps less hyena-like than it is in the lower series. The carnassials in each, of course, are not homologous. The upper cheek tooth series in Patriofelis ferox was described by Matthew (1909), but the anterior part of the dentition was not known. The University of Utah specimen demonstrates that there are only two upper incisors and that M? may be present so that the formula for the genus may be written pee cs Panu, 2-3? I 3 2 with M? and M, as carnassials. The upper incisors are simple teeth with conical crowns exhibiting enamel distributed a little higher on the outer side, and a prominent lingual cingulum that is carried nearer the apex of the crown medi- ally. The median incisor is comparatively small with a transversely flattened root, whereas the lateral of the two is decidedly large and more caninelike in appearance. Its root is more nearly circular in cross section, but with the posterolateral surface somewhat flattened. The canine is very robust and heavy rooted, approximately oval in cross section—not flattened or saberlike. These teeth have been much blunted by wear. There is no Pt. P? is simple and two rooted with a very broad I4 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 posterior portion. There is a small posterior cusp placed buccally and a brief shelf posterolingually, but without a deuterocone. P® is three rooted with a small anterior cuspule and a large tritocone not as high as the primary cusp. The deuterocone, though damaged, is seen to be well developed and about median in position. In P* the small an- terior cusp is higher or nearer the apex of the primary cusp and the tritocone is about as large as the primary cusp but more bladelike in appearance. The talon carries a well-developed crestlike deuterocone and is anteroposteriorly broader and more anterior in position than that of P*. M?’, the carnassial, has been converted entirely to a shearing blade. This tooth is rather worn lingually, but it is apparent that the anterointernal root did not support a talon or deuterocone. M? is a small peglike tooth anterolingual to the posterior margin of M?. An interesting feature of the Patriofelis upper dentition is the ex- tent to which it is carried outward and posteriorly on the strong zygoma as in cats and hyenas, and the fossil form, Hyaenodon—quite unlike the bears, and possibly dogs. Also, as noted by Matthew (1909), the upper cheek teeth are inclined inward, very much so in the posterior part of the series, so that the shearing surface, particularly of M?, is vertical. The outer wall of M? is nearly horizontal and the angle that it makes with the shearing surface is, in consequence, not particularly acute. Also, as a result of this, the vestigial M* is im- planted at an angle, dorsal to the crown of M7’, so that it is almost concealed in the ventral view. Its small crown scarcely reaches the plane of shear on M, immediately ventral to it. Mandible—The Patriofelis jaws (pl. 4), as Matthew (1909) has noted, are deep and massive. The symphysis is deep and elongate, and although Matthew considered it as not co-ossified, I find the two rami are firmly united. When it was necessary to separate the jaws so as to remove them from the skull during preparation, breakage for the most part occurred to one side through the canine alveolus. The anterior margin of the symphysis is a little less abrupt than Matthew has shown for P. ferox, curving gently into the comparatively straight lower margin of the horizontal ramus. The depth of the jaw be- neath the tooth row is nearly uniform, though a little shallower be- neath the posterior root of P, as shown for P. ferox. The mental foramina are variable and on the right side two are located one above the other beneath the anterior part of P., and two side by side be- neath the posterior root of P; and the anterior root of Py. On the left side two slightly larger foramina are located, one beneath P, and the other beneath P;. There is also an irregular display of foramina beneath the incisors close to the anterior margin of the symphysis. , no. 8 SKULL OF BRIDGER CREODONT—GAZIN 15 Neither the angle nor the top of the coronoid process are complete on either side of the P. ulta mandible, but it is seen that the slope of the anterior margin of the ascending ramus is not so steep as shown for P. ferox. The condyle is transversely very elongate and carries the articular surface well forward along the inferior as well as the superior surface. The outer portion of the superior surface extends down on the anterior part of the condyle where articulation occurs with the well-developed process anterior to the glenoid surface of the squamosal, almost locking the lower jaw in place, as in some mustelids. The masseteric fossa would appear to be weakly defined near the lower margin of the jaw but is deeply impressed in the upper portion. The deeper part of the fossa is limited downward by a ridge which extends forward from just below the condyle. The crest bounding the fossa anterodorsally extends downward and forward from the anterior margin of the coronoid process, but disappears upon reaching a position almost below the posterior margin of Ms. On the medial surface of the jaw it is seen that the symphysis ex- tends posteriorly to a position below about the anterior margin of P, and exhibits a deep pit forward near its posterior limit for certain muscles, including the geniohyoid and probably a part of the digastric. The inferior dental foramen is located above the shallow vascular notch in the lower border of the jaw and about opposite the ridge on the outer surface that limits the deeper part of the masseteric fossa ventrally. Posterior and ventral to the inferior dental foramen the medial surface of the jaw is distinctly concave. There is no particu- lar indication of a sulcus mylohyoideus. Lower dentition—As noted above, the hyena-like appearance of the teeth (pl. 4) in Patriofelis is most noticeable in the lower series, particularly the premolars. The resemblance in the molar series is be- tween nonhomologous carnassials and is upset by the presence of the small M, in Patriofelis. The number of lower incisors is clearly two in the University of Utah specimen. The smaller, medial incisor is distinctly posterior to the lateral tooth and rather flattened transversely. The lateral incisor is less procumbent and shows a relatively broad anterior surface. The crowns of both are blunt with wear. The canines have massive roots and are comparatively close together, much crowding the incisors. Their crowns are likewise considerably worn. P, is neither crowded nor oblique as in P. ferox. It shows a short diastema between it and the canine, and though small, is relatively broad and two rooted. It carries a minute cuspule anterior to the principal cusp and a low, blunt cusp on the talonid. Ps is similar but 16 SMITHSONIAN MISCELLANEOUS COLLECTIONS VOL. 134 much larger and broader, with a relatively larger and transversely flattened talonid cusp. Like P,, this tooth shows a distinct backward tilt. P, is larger than P; and has higher cusps, also the talonid shows a more pronounced crest on its lingual margin. The backward tilt of this tooth is rather pronounced, so that the outer margin of the talonid is much lower than that of the trigonid, or than any of the other teeth. M, is small and crowded with a comparatively large paraconid por- tion, although this part of the tooth is rather obscured by wear. The metaconid is developed as an upward and posterolingually directed spur from the protoconid. The talonid is low, much worn, and almost completely hidden lingually by the anterior root of My. Mz, of course, is the shearing tooth and possibly a trifle longer than P,. It lacks any trace of a talonid. The posterior blade along its cutting edge is longer than the anterior, and projects backward and upward rather strikingly. In addition to the backward tilt noted for P; and P,, all the cheek teeth, as noted by Matthew (1909), tilt distinctly outward. As with the inward tilt of the upper teeth, this orients the shearing surface of P; and P,, as well as that of the carnassial, nearly vertical. It is noted also that the outer shearing surfaces are dorsoventrally more elongate than the lingual walls. The crown of each tooth has a noticeably greater buccal than lingual height. MEASUREMENTS IN MILLIMETERS OF SKULL AND MANDIBLE OF Patriolefis ulta LEIDY, UNIV. UTAH NO. B50 Skull: Greatest length from anterior margin of premaxillae to two small processes on superior margin of foramen magnum...... 248. Length from anterior margin of nasals to vertical portion of Occipit above, fOrdiien MARI. 66S. dads ovelecseesciaesee 227. Length from anterior margin of premaxilla to posterior wall of glenoid curitee/mediallis ci 2 sei. Ae ee DAVE IN COLO 178. Length of palate from anterior margin of premaxilla to anterior MARS OPMPOStGhiOL NAviAl APELFEULE.. 4 ajc,0c0.6 6 0:6.5:<0,0.6:0te sia vn are 100.5 MME CRY, NEGHEUIN ON MS ASAIS Ge Le EMU ih gic Use nih coiaen os legs «oni 78.0 Distance between lateral margin of anterior narial aperture and Gnterion Matear OF OLbil. foc stak eee eek s &E Es. Gilet 52.5 Crreatest) width across: sy pomiae) 2.256 iss sé ews sies hei enwns 183. Waar merce pagals ANtSTION ys. jo wyeiwid oye wibyeisya «dem acd cls mains aera 40. Wy tte MEEWEEN “OFPItS GOLSAILY 5 ooo ai. occ 6 susiee cs bveesee ves occa''e 76. Width across postorbital processes of the frontals.............. 70. Mista of teraniuim ‘at COnsirictione.s 2. le... i vse bese sal eee ee 38. Width of palate between canines: 1.2.0. ocd cde ocssclcccs scans Kite Width of palate posteriorly, between M?’s at alveoli........... 81 Upper dentition: Over-all length of dentition from anterior surface of lateral picisn to posterior tdatein Of Mt... os cscsass od aceccaueesg 105. no. 8 SKULL OF BRIDGER CREODONT—GAZIN 17 Length of cheek tooth series, P?-M}, inclusive................+ 68.5 I? (at alveolus), anteroposterior diameter: transverse diameter. . 9.0: 4.0 I? (at alveolus), anteroposterior diameter: transverse diameter.. 13.0: 10.0 C (at alveolus), anteroposterior diameter: transverse diameter.. 23.0: 16.0 P2, anteroposterior diameter: transverse diameter posteriorly... 11.2: 8.0 P3, anteroposterior diameter externally: transverse diameter per- pendicular’ toy outetawalll: jas sige dee «kiiaee ce aac aa ower eres 17.8: 19.0% P4, anteroposterior diameter externally: transverse diameter per- DENGICT ate TOPOULER, Wall ys ots) c.cve, je ycpalcre'eisis <:5l