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UNITED STATES DEPARTMENT OF THE INTERIOR
SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY 1931
GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 UNITED STATES DEPARTMENT OF THE INTERIOR Bay Ljrman Wilbur, Secretary GEOLOGICAL SURVEY W. C. Mendenhall, Director
Professional Paper 170
SHORTER GONTRIRUTIONS TO GENERAL GEOLOGY
1931
T. W. STANTON, CHIEF GEOLOGiar 1
UNITED STATES GOVERNMENT PRINTING OFFICE WASHINGTON : 1932
Far sate by the Superintendent of Documents, Washington, D. C.------Price 35 cents CONTENTS
[The letters in parentheses preceding the titles are used to designate the papers for advance publication]
Page- (A) Glaciation in Alaska, by S. R. Capps______^______-______-.______1 (B) The Upper Cretaceous ammonite genus Barroisiceras in the United States, by J. B. Reeside, jr______Q (C) A Miocene flora from Grand Coulee, Wash., by E. W. Berry______31 (D) Pliocene fossils from limestone in southern Florida, by W. C. Mansfield______43 (E) The geologic importance of the lime-secreting algae, with a description of a new travertine-forming organism, I y M. A. Howe ______57
ILLUSTRATIONS
PLATE 1. Sketch map showing the largest of the existing glaciers in Alaska, areas covered by glacial ice during the Wis consin stage of glaciation, and localities at which possible evidences of pre-Wisconsin glaciation have been found______In pocket^ 2. Sketch map showing the lines of flow in the Wisconsin glaciers of Alaska and position of the 100 and 50 fathom contours in places along the southern coast______In pocket. 3-10. Species of Banwsiceros______-____-__-______-_--_-__-______22-29 11-13. Miocene flora from Grand Coulee, Wash______-__-__-_-__-_____--__------_-______..__ 42 14-18. Pliocene fossils from limestone in southern Morida____-___-_---_--_-______.._----__---_-___-______52—56- 19-23. A new travertine-forming organism______65 PIGURE 1. Typical section of peat and glacial till on White River, Alaska, 8 miles below the terminus of Russell Glr
GLACIATION IN ALASKA
By STEPHEN R. CAPPS
INTRODUCTION examination. Interior Alaska, on tke other The history of glaciation in Alaska offers a fas presents a great driftless area, in the basins o* the cinating field for study. Because of the remarkable Yukon, Tanana, and Kuskokwim Rivers, where low development and easy accessibility of valley and pied relief and dry climate prohibited the formation of mont glaciers in the coastal mountains, Alaska has glaciers. This unglaciated region was encrorehed long been popularly conceived as a land of ice and snow, upon by the continental ice sheets from the eas* and a concept that is only slowly being corrected. To by mountain glaciers from the north and s^utfe. the student of glaciation, however, Alaska affords a Along its margins at several localities there have unique opportunity to observe the formation, move already been found evidences of glacial advances ment, and dissipation of the many living glaciers, to preceding the last great glaciation, and it seems ee^ain examine the results of glacial erosion on a gigantic that future studies will bring additional observa tieas scale, and to discover and work out the sequence of that will shed much light on the glacial history cf the Pleistocene events as shown by the topographic forms continent. in both glaciated and unglaciated areas and by the * There is an extensive literature on glaciation in deposits left by ice and water during earlier stages of Alaska, yet in view of the great area of the Terrf.tory, glaciation. the number and size of its living glaciers, and the The evidence for successive glacial advances in extensive area covered by ice during Pleistocene time, many parts of the world during Pleistocene time has it must be confessed that little more than a beginning been largely obtained in regions not far from the outer has been made toward an adequate understanding of margin reached by the glaciers during the different its glacial history. Each year since 1898 there have stages. This is necessarily so, for that evidence been a number of Geological Survey parties in the field, consists mainly of the superposition of till deposits engaged for the most part in reconnaissance or erolor- and their relations to one another, to preglacial, inter- atory surveys, with the result that about Jbitlf the glacial, and postglacial deposits, and to outwash Territory has been mapped, and a fair knowledge of materials laid down beyond the ice edge. Morainal the extent of glaciation in the surveyed areas has been deposits are best developed near the margins of obtained. Many descriptions of living glaciers have glaciated areas, and it is therefore in such areas that also been published, and Tanr and. Martin, as the result observations having a significant bearing on recurrent of three years of study under the auspices of the glaciation are most likely to be made. National Geographic Society, prepared an imposing Alaska would thus seem to be a promising region volume la that deals largely with the living girders for the study of the events of Pleistocene time. The along the Pacific coast and the lower Copper Fiver. Territory lies just west of the border of the great The literature is widely scattered, however, aad it continental ice sheet, and although it was never itself seems worth while to review our present knowledge of overridden by glaciers of the continental type, its the subject. The details of mapping; as shown in the climate so closely approached that necessary for con illustrations presented herewith, are in large part taken tinental glaciation that all the higher mountain masses from the observations of members of the Alf«*kan were severely glaciated. From the coastal mountains branch of the Geological Survey. along the entire Pacific littoral of Alaska 1 glaciers EXISTING GLACIERS descended to the sea. There, unfortunately, the evi Existing glaciers in Alaska cover an area of less than dence of the limits reached by the ice edge, as displayed 20,000 square miles, or slightly more than 3 per cent by moraines, is submerged and not available for direct & Tarr, R. 8., and Martin, Lawrence, Alaskan glacier studies,408 pp., Na^, Geog. i As used in this paper the term " Pacific " does not include Bering Sea. Soc., 1914. 1 SHOETER CONTRIBUTIONS TO GENERAL, G1OLO&Y of the total area of the Territory. Plate 1 shows the largest area includes the Pacific coastal region, and largest of these glaciers, but there are probably several embraces all of southeastern Alaska, tH Chugmeh, thousand small glaciers, from a fraction of a mile to Wrangell, Talkeetna, and Kenai Mountains, the several miles in length, that lie in unsurveyed areas or Alaska Range and it® southern extension into the are too small to be shown on a map of this scale. The Alaska Peninsula, ami tfa« greafc basins o* the .Copper glaciers are almost exclusively confined to the coastal and Susitna Rivers and upper Cook Inlet. Next in mountains, the Wrangell Mountains, and the Alaska size was the great glacier that occupied the entire Range. This distribution is in large part a response Brooks Range, in northern Alaska. The other areas to high topographic relief but in part also to heavy in which glaciers occurred are scattered throughout precipitation. The coastal mountains reach altitudes central and southwestern Alaska and Seward Penin of 15,300 feet at Mount Fairweather, 18,008 and 19,850 sula, and all are small. feet at Mounts St. Elias and Logan, and 6,000 feet in The great ice mass that occupied southern and south the southern part of Kenai Peninsula. The Wrangell eastern Alaska, though connected toward the east with Mountains have many peaks of 12,000 to 14,000 feet, the continental ice sheet, was entirely independent of and the more heavily glaciated portions of the Alaska that sheet as to its source of ice supply, the directions Range reach 10,000 to 11,050 feet near Mount Spurr, of ice movement, and its persistence. It was fed 13,740 feet at Mount Hayes, and 20,300 feet at Mount solely by glaciers that had their origin within its own McKinley. In the Brooks Range few peaks reach area, and its lines of flow were directed ty the moun altitudes of more than 8,000 feet, with a possible tain topography within that area. Throughout Alaska maximum of 10,000 feet. The most active centers of as a whole the balance between temperature and glaciation to-day are therefore in places where high precipitation was such that glaciers could form and mountains lie within areas of heavy rainfall, as along grow only in the higher mountains, and e^en there the the coast. High mountain areas of moderate rainfall size and vigor of the glaciers depended in large degree are represented by the Wrangell and Talkeetna Moun upon the abundance of precipitation. Th«, distinction, tains, which cany less extensive glaciers, and by the therefore, between the Alaska glaciers p.nd the con Alaska Range. The fairly high mountains of the temporary continental glaciers in former stages of ice Brooks Range, lying in a belt of scanty precipitation, expansion was that in Alaska each of the larger glaciers have only a few small glaciers. That the extent of was formed by the coalescing of a great number of glaciation in past times was strongly influenced by the individual valley glaciers, each of which responded to amount of rainfall, as it is to-day, is certain, and a the accretion of ice within its own basir and moved realization of that fact is important to the understand down its own mountain valley in a way the,t was largely ing of the peculiarities of ice distribution during the independent of the movement of its neighboring ice last great ice advance in Pleistocene time. streams. It was only because these adjoining moun For size, accessibility, and beauty the coastal glaciers tain glaciers grew to so large a size that tiNy coalesced of Alaska are in many ways unique. They have been to form nearly continuous ice caps. E "en at their studied by many competent geologists, and much has maximum, however, there were high peal's and divid been written about them. Data concerning their ing ridges that separated them from one another, and movements are rapidly accumulating, and during the it was only in those places where the individual ice summer of 1929 the lower portions of nearly all the streams emerged from the mountains onto the lowlands larger glaciers of southeastern Alaska were photo that they joined and lost their individuality. graphed from the air. These photographs will prove In Plate 2 an attempt has been made to show the invaluable for the purpose of checking future changes lines of flow in the two larger glaciated areas. The in the positions of the ice fronts. Any adequate arrows indicate th» direction of flow of various threads description of the hundreds of imposing glaciers of of ice within the areas where the ice formed a prac Alaska is far beyond the scope of this paper, but it tically continuous cap, with only the Mghest peaks and should be kept in mind that the glaciers of to-day are ridges projecting a-bove its surface. The dotted'lines but the shrunken remnants of the much greater glaciers indicate the divides between the glaciers that moved of the past, that they have probably existed continu south and those that moved north, and w^st. ously from Wisconsin time to the present, and that In southeastern Alaska, south of Cros^ Sound, the many high valleys may have been continuously occu threads of flow had in general a southerly direction, pied by ice since early Pleistocene tune. being influenced by the preglacial topogr-aphy, which in turn was determined by the trend of the rock FORMER GLACIAL ADVANCES structure. I know of few more striking physiographic Plate 1 shows the areas in Alaska covered by glacial features than the great fiord formed, by Chatham ice during the last great ice advance. During the Straits and Lynn Canal, cutting obliquely across a time of maximum glaciation there were in Alaska two rugged mountain region in a straight line for 250 major areas of glaciation and many smaller ones. The miles. The riddle of this great fiord has not yet been GLACIATION IN ALASKA entirely solved, but it is known that a great preglacial Tanana River. The waters from the melting Delta structural valley was widened, deepened, and straight Glacier therefore flow at times by way of the ened by ice scour and that faulting had much to do River to the Pacific and at tames by way of the with the establishment of the preglacial drainage lines. tributaries to Bering Sea. On occasion the st-eam On the southern slope of the St. Elias, Chugach, and splits, part flowing one way and part the othe^-, eo Kenai Mountains the ice threads in general followed that a salmon could conceivably ascend the Cc*>per direct courses to the sea. On the inland slopes more and Gulkana Rivers, enter the head of the Delta and complex flow patterns were developed. Between the descend to Bering Sea, crossing a great mountain arc of the Chugach Mountains, which form a barrier range on the way. along the coast, and the great curve of the Alaska In Plate 2 the dotted line indicates the divide betr^ai Range, farther north, there is a region of milder relief the ice streams that drained to Bering Sea and those containing the basins of the Susitna and Copper that sent their waters to the Pacific. In a general Rivers but broken by two separate mountain groups, way this divide follows the crest of the Alaska Range. the Wrangell and Talkeetna Mountains. Into these As plotted it ignores the ice spillways through tfa® basins ice poured down from all. the surrounding range at the passes noted above, as it is impossiF^^ highlands and from the Wrangell and Talkeetna Moun estimate how large an area of the ice in Copper md tains as well, until the lowland was filled with ice Susitna Basins drained northward through these that sought outlets through the gaps that offered passes. For a part of the way the ice divide fo%ws themselves. The lowest outlet to the coast was by way the crest of the Wrangell Mountains, whose northward- of the Susitna Basin, toward which most of the threads flowing glaciers crossed the Nutzotin Mountains of flow converged, but at the time of maximum ice through the eanyoBS of the Nabesna and Chisana development lobes spilled over the basin margins into Rivers. the valleys now occupied by the Copper, Nenana, A striking fact is the meager development of the and Delta Rivers, through Mentasta and Suslota Pleistocene glaciers on the north side of the Alaska Passes, and probably also into the valley of the Range between the Tonzona River and Mentasta Nabesna River by way of Jack anc^ Platinum Creeks. Pass as compared with those on its south side. TMs Through the rim of the intennontane basin these same discrepancy is shown, by the glaciers of to-day. overflow lobes eroded deep valleys, which were later It is due in part to the asymmetrical position o* the utilized by the draining streams of the glaciers as the crest of the range. On the north slope the moun^ins ice shrank in retreat. This eventually resulted in the rise steeply from the lowlands to the summit capture, by the Copper, Nenana, and Delta Rivers, of and the belt of high mountains in which ice drainage areas within the intermontane basin, and we lation can take "place is narrow. Furthermore now have the unusual condition of rivers draining mountain glaciers within a few miles of their source mature headward basins through youthful canyons move out into a relatively low, arid lowland, vibe*® carved directly across high mountain ranges. Al dissipation is rapid. By contrast, the mountaia belt though the Copper River now drains a large area on the south side of the range is wider from the d*TM© between the Chugach and Alaska Ranges, it is quite to the lowlands, there is a greater area, for ice aee^mii- evident, from the topographic youth of the part of its lation, and the basins into wMeh the glaciers m^etge valley cut through the Chugach Mountains as com are higher and less arid. A second fact, perhaps of pared with the maturity of the part north of the equal importance, is the difference in the amount of coastal range, that the drainage discharge from the precipitation on the two slopes. No accurate records upper basin of the river formerly found some other are available for points on the mountain slopes, but course to the sea. That course doubtless was by way throughout the Susitna Basin as a whole the avmge of the Susitna Basin and probably lay north of the precipitation is several times as great as in the Tanana Talkeetna Mountains. The working out of this great Basin. The winds that strike the Alaska Range from change of drainage has been complicated by Pleistocene the west have already passed over several hurdred or post-Pleistocene warping, and the details are not miles of dry, rolling country and have lost a consider yet known. able part of their moisture content. The moist triads Another anomaly occurs at the head of the Delta from the Pacific, on the other hand, blowing up Cook River, which has its origin in a large glacier. That Inlet, are trapped between high surrounding inotai- glacier lies on the south slope of the Alaska Range and tains and drop much of their moisture on them. would normally be expected to drain to the Copper The great ice cap that covered the Brooks Isange River. The Delta River has built up a gravel train was likewise independent of the continental iee sheet that splits, a part sloping southward toward the in supply and in direction of movement. It m*y or Copper River and a part draining into the Delta, which may not have been connected with the contau^otal flows northward through a narrow glacial valley sheet near the mouth of the Mackenzie River, The directly across the Alaska Range to empty into the Brooks Range lies in a difficultly accessible piH of SHOBTER CONTRIBUTIONS TO GENERAL 0EOL.OGY, 19 SI
Alaska, and the geologic studies made there have all to that now found along the borders of the Antarctic been of reconnaissance or exploratory character, so Continent. It seems to me very likely that such a that many details of its glacial history are yet un barrier did exist. Plate 2 indicates the position of the known. The outline of the glaciated area as shown on 100-fathom contour along this coast. At most locali Plate 2, however, is believed to approximate the ties where large valleys emerge at the cc *ist there are truth. Like the great ice cap to the south, this one deep channels across the continental shelf, such as was composed of numerous valley glaciers which flowed those between Afogoak Island and the mainland of out radially from the mountains but which at the time Kenai Peninsula; at tile entrance to Prnce William of their greatest extent filled adjoining valleys and Sound between Hmehiftlarook and Mant^ue Islands; coalesced to form a nearly continuous ice cap, above and at Yakutat Bay, Cross Sound, ChrStian Sound. whose surface only the highest summits projected. In Iphigenia Bay, and Dixon Entrance. The formation general, the southward-flowing ice threads appear to of these channels seems to demand some ftrong erosive have been longer than those that flowed to the north. force, and glacial ice is known to have mc^ed out from The direction of flow of each thread was entirely con shore at many if not all of these place'. Tarr and trolled by the topography of its mountain valley. Martin 2 concluded that no ic© more than 400 feet Between the northern and the southern ice caps thick issued out to sea between Hinchinbropk and Mon have been found about a score of localities in which tague Islands, basing this conclusion up^n the height glaciers of minor extent existed during the time of the to which they found erratic boulders on the south end last great ice advance. All but one or two of these of Hinchinbrook Island. They also concluded that places consist of a high mountain or group of moun ice passing southward along tfe© west shore of Montague tains upon which one or two small valley glaciers were Island barely issued into the open sea. I am inclined able to form during the period of maximum glaciation. to doubt the validity of their conclusions on these These glaciers were comparatively short-lived and points. A study of the glacial smoothing on the south have now disappeared entirely. A single area of con end of Hinchinbrook Island, as seen from a ship pass siderable size is that lying between Bristol Bay and ing into Prince William Sound, seems to irdicate rather the lower Kuskokwim River, where such scanty infor distinctly that ice scoured the south end of that island mation as is at hand indicates a center of notable to a height of several times 400 feet, at least. The mountain glaciation. 100-fathom channel extending southward from that Plates 1 and 2 portray the distribution of glaciers entrance certainly suggests glacial erosion of the bot in Alaska during the Wisconsin glacial stage in so far tom, and reported deposits of glacial till and boulders as they covered land areas. An interesting but more on Middleton Island indicate the possibility that we difficult problem is that of determining how far the pushed out some 60 miles to sefc across thn shoal within ice of southern and southeastern Alaska pushed out the 50-fathom line, shown, on Plate 2i< to sea at that time. An examination of maps of the At a great number ol places within tfee glaciated Antarctic ice cap and the adjacent ocean basins shows areas of Alaska observations have been ir^ie as to/the that the ice barrier there, in places where its face is thickness reached by the,ice during the time of maxi 50 to 80 feet high and its thickness therefore not more mum PleistiM|jiRfst gbeaatioii. This information is 'than 400 to 600 feet, projects out into oceans that are difficult to sbaw «ion; the abundance of polished and striated rock to the stream level and are gradually thawo4 ia«l surfaces and erratic boulders in a region where ex removed. foliation and weathering are rapid; and the unoxidized The peculiar appearance of the roots of the spruce character of the glacial till all point to a relatively trees that grow on the edge of the bluff and of the recent date for the last great glaciation. All such stumps that occur through the peat deposit sufrg®«t©«t evidence indicates comparative youth but is not suf that it might be possible to determine approximate^ ficient to assign to these phenomena an age stated in years. In the basin of the White River, near the interna tional boundary, however, excellent exposures along a newly cut river bluff reveal evidence that makes it possible to date rather accurately the time of the glacial retreat past that place.3 The locality is not FEET far from the source of the river in Kussell Glacier. P»at7' This glacier is a large and vigorous ice stream that Volcanic ash 2' draws its ice supply from the high mountains of the -60 Wrangell and St. Elias group. It may fairly be con sidered an average example of the glaciers of that -BO region, and its history must have been much the same -4O «s that of similar glaciers in that part of Alaska. About 8 miles below Kussell Glacier, on the north bank of the White Kiver, that stream has cut a bluff •over a mile long and 50 to 70 feet high. A typical -20 section there exposed is shown in Figure 1. At the base of the bluff is 30 feet of unconsolidated and un Glacial till oxidized glacial till, with an uneven, rolling surface. Above the till and extending to the top of the bluff is *-© 39 feet of fibrous, peaty vegetable material, full of spruce stumps and roots but composed for the most part of the remains of sphagnum moss. This heavy FIGUKE 1.—Typical section of peat and glacial tfll on th* White Biwv Alaska, •deposit of peat is interrupted, some 7 feet below the 8 miles below the terminus of Russell Glacier top of the bluff, by a 2-foot layer of white volcanic the rate of accumulation of peat at this place and so ash. The surface of the bench, back from the bluff, determine the time that -has elapsed duo© the ice is covered with living sphagnum moss and a dense withdrew from ita moraine her© and thus per^tect forest of spruce trees. At the time of visit, in July, reforestation. The ordinary spruce tree, gwpiag ou till, peat, and ash were frozen within a few inches of solid ground, either frozen or unfrozen, sends it* r©&te the surface along the face of the bluff, and in the out radially, parallel with the surface of 4he pnouad forest permanent ground frost was found 6 inches and only a few niches below the surface. (Se6 %. 2.) Uprooted stumps of this kind are a fwmMar sight. In the White Biver Iocalit7 here described, however, the roolas of the spruce trees, both those growing at the e%e of the bluff, or recently; overturnec1 , and those deeply buried witliin tjbe peat mag®, show quite different characteristics. In stead of a single, fiat-based set of radial roots, each of these trees shows a central stem, a sort of taproot, from which radial .—Diagrams showing the character of the roots of a spruce tree (A) growing normally on solid roots branch off at irregular intervals, ground and (B) growing on rapidly forming peat, White Eiver, Alaska with-an upper set of roots near tie sur beneath the surface of the growing moss. The cut face corresponding to those of the normal tree. bank has a vertical to overhanging face, and erosion Around the living trees the ground was frozen 6 inches takes place by the formation of great, clean vertical below the top of the moss. Below the frost lr*e the cracks through the frozen peat and the falling out roots were sound and undeeayed, but they wer** of a ward of large tree-covered blocks, which tumble down darker color than the Eve surface roota and wr*e ap 8 Capps, S. R., The Chisana-White Eiver district, Alaska: U. S. Geol. Survey parently not functioaing. It is evident th$t the living Bull. 630, pp. 69-75, 1916. tree derives its nourishment from the groutM* only 6 SHOBTEB CONTRIBUTIONS TO GENEBAL. GEOLOGY, 1931 through the roots in unfrozen ground near the surface, of shrinking than during the later stages. For the and that the lower roots cease to function as soon as last 35 years the ice edge has remained practically the line of permanent frost rises above them. stationary. From the facts stated above it appears that a seed Various estimates have been made of the length of ling spruce, having established itself on the mossy time since the Wisconsin continental ice sheet "began soil of this area of rapidly accumulating vegetable its retreat, but the consensus of opinion se<*tjas to place material, sent out a set of radial, flat-based roots in that time as somewhere between 80,000 and. 60,000 the ordinary way, but the constantly thickening moss years. The determination made in the ""lute River and the consequent rise in the level of ground frost Valley, at a point that was not bared until a large part cut off the food supply from the lowest roots and of the retreat had been accomplished, is of the same forced the tree, in its efforts to survive, periodically order of magnitude, and it seems safe to say that the to throw out new sets of roots into the unfrozen sur last great ice advance in Alaska was contemporaneous face soil. If these premises are correct, then the with the late Wisconsin continental glaciation. vertical distance between the lowest set of horizontal roots of a living tree and the surface of the ground PRE-WISCONSIN GLACIATION represents the thickness of the peaty accumulation As the last great glaciation in Alaska is thus regarded during the lifetime of the tree, and the rate of accumu as of late Wisconsin .age, the question arisen as to what lation can be determined by ascertaining the age of were the conditions in this region during the earlier the tree, as shown by the annual rings. stages of Pleistocene glaciation elsewhere on the con Any figures for the rate of accumulation of the peaty tinent. Information on that question muH be sought deposit that were obtained in the way outlined are mainly in the superposition of glacial and interglacial subject to a number of uncertainties. Most of the deposits, and in a frontier country where road, railroad, qualifying factors, however, fall on the side of con and other extensive excavations are few and where little servatism and result in a minimum rather than a more than a beginning has been made in the study of maximum figure. , Among the unweighed factors is such subjects, facts that bear on this protlem come to the possibility that the peaty material is compressed light only infrequently. Furthermore, there is evi after burial. The amount of such compression, how dence in Alaska, where the Pleistocene glaciation was ever, is probably very small, for the peat is perma almost entirely mountain glaciation, that the last ice nently frozen within a foot or less of the surface and advance was more vigorous than the earlier ones, has remained so since its formation. Another factor with the result that the last glaciers destroyed much that might affect the rate of accumulation is the of the evidence of the work that may have been done quantity of wind-blown sand, which is noticeably by their predecessors. Nevertheless, at several local present near the edge of the timbered bench. ities evidence has been found of Pleistocene glaciation Throughout the deposit as a whole, however, the that antedated the ice of the Wisconsin stage. (See* percentage of wind-blown material seems to be fairly pl.l.) uniform. Other elements of uncertainty appear to Qa the southern flanks of the St. Elias Mountainmass be of so small importance as to affect the calculation there occurs in tlie Oiaix Hills, m described1 by Russell,4 but little. and in the Robinson Mountains, as demerit M by Mad- From ring counts on a number of trees and from dren,8 a tMekaess of 2,000 to 5,000 feet of beds that measurements of the distance between the lowest and are, im part, at least, of glacial origin, and that cany uppermost radial roots on the same trees, it was Pleistocene marine fossils. These beds are now up determined that the peaty material is now accumulat lifted to altitudes as great as 5,000 feet and are inter ing at a rate of about 1 foot in 200 years. It seems esting in showing the active growth of the St. Elias that this factor may be safely applied to "the whole Mountain mass. As evidence of a glacial stage earlier thickness of 39 feet of peat, from which we arrive at than the Wisconsin, however, they have less signifi a figure of 7,800, or, in round figures, 8,000 years since cance, and unless a more accurate determination of the the- ice of Russell Glacier withdrew beyond this point. age of the inclosed fossils can be made, their correlation Even if this figure is admitted to be 50 per cent in must be vague, Both these ranges of Mils lie within error, it still gives a basis for calculation. an area that ia even new severely glaciatHl, and they At the time of its maximum extension Russell are at least partly surrounded by the greH piedmont Glacier, according to Hayes, extended northeastward ice lobes of Bering and Maiaspina Glaciers. In about 130 miles beyond its present terminus. Its other words, that area of high mountains is even now retreat to the peat deposits described above, which in a glacial period «ad may well have ensured glacial lie about 8 miles below the end of the present glacier, conditions continuously since the beginning of the was therefore 94 per cent of its total retreat. So far 4 Russell, I. C., Second expedition to Mount St. Bliss, ia 1891: IT. S. Oeol. Survey as time is concerned, it is quite possible that the glacier Thirteenth Ann. Bpt., pt. 2, pp. 2*-26,1898. 6 Maddren, A. G., Mineral deposits of the Yakataga district: U. S. Geol. Survey- retreated much more rapidly during the earlier stages Bull. 562, pp. 131-132, 1914. GIACIATIOBT ALASKA Pleistocene epoch or even longer. The glacial beds indicate that during some pre»Wisconsin glacial of the Robinson and Chaix Hills are therefore as likely a vigorous ice tongue pushed northward from th<* range to have been laid down during a time of small ice at least 25 miles farther than the Wisconsin!^ and development as during a time of ice expansion and that at the point where the Wisconsin ice tenr%at®d thus can not be correlated with any definite stage of the older glacier had a thickness of at least 2,fW^ feet,' Pleistocene glaciation. Although the erratic boulders left by this earlier glacier Another locality at which evidence of glaciation have suffered somewhat from weathering and, «re less Antedating the Wisconsin has been found 6 is in the fresh in appearance than glacial boulders of valley of the White River, 5 miles north of the snout of age, they are nevertheless still firm and little Uussell Glacier. Foothills adjoining the main moun and are more likely to belong to a late pre*WimMBisi tain mass of Carboniferous lavas and sediments show a stage than to an early one. section of more than 3,000 feet of tilted beds of glacial Still another locality at which evidences off^-Wis*- and glacio-fluvial origin. Ten distinct beds of tillite consin glaciation have been found is oil the wee *i fttak or of till were recognized, separated by beds of gravel of the Alaska Range, in the basin of the Muhaatna and of finer clastic sediments. Most of the beds of River. During the summer of 1929 the writer found till have been indurated to form hard tillite and have there a deposit of deeply oxidized and wer tfaered been etched into high relief by erosion. They contain material that in composition, lack of assortment, and abundant beautifully striated and faceted boulders, shape of included boulders and blocks seems ceHainly cobbles, and pebbles. In places the tillite was over to represents glacial moraine. The included boulders ridden and smoothed by glacial ice during the Wisconsin and rock fragments, however, are aH so weat&erxi and ice advance. It is, therefore, old enough to have been decomposed that their original surfaces have been lost. indurated, uplifted, and eroded before Wisconsin time. No striae were found, but few of the rocks were firm It is impossible, with the information now at hand, to enough to retain striae. I believe this deposit to be a correlate this older glacial material with any definite remnant of an ancient glacial moraine. It is now stage of Pleistocene glaciation. Indeed, there is no overlain by several hundred feet of fresh, ti&OTidized positive evidence that it is of Pleistocene age, though glacial till that forms a lateral moraine left by the I am inclined so to assign it. Certainly it greatly Wisconsin glacier. This weathered deposit also, antedates the Wisconsin stage. In view of the known though certainly representing a stage of Rektocene activity of mountain growth in this part of Alaska, the glaciation older than the Wisconsin, can rnt be uptilting could have occurred in Pleistocene time, and definitely correlated with any particular glacial stage. comparatively recent volcanism in this region, together SUMMAKY OF KNOWN FACTS CONCERNING FBI- ivith the stresses of tilting, may have resulted in the WISCONSIN GtACIATION IN ALASKA induration of some of the beds. As regards the evidence from this locality in respect to The main purpose of this paper is a diseusnon of the extent of the glaciation represented by those beds, Pleistocene glaciation in Alaska, but it seems well to no great extension of the ice from its present stand mention briefly here reported occurrences cf pre~ would be required to reach the localities where the Pleistocene ice invasions. older tillite occurs. Indeed, the whole aspect of this Cairnes 7 in 1914 described a conglomerate, & ought deposit suggests that it may have been formed near by him to be of Carboniferous age, occurring at a the oscillating edge of a glacier, repeated advances locality on the Alaska side of the international I^ound- being represented by layers of tiH and retreats by ary just north of the Yukon River. He thougl t that deposits of gravel, sand, and silt. The deposit can this formation might be of glacial origin, though he be said to show only that glacial conditions existed admitted that the question was stall open. Mertie,8 in that part of Alaska at some time long before the after later studies of th& same formation, determined Wisconsin advance. its age to be Cambrian or pre-Cambriaa and con A third area in which older glacial deposits have cluded that its glacial origin was not yet established. been found occurs along the valley of the Nenana If this material is glacial, it represents the oldest River, some distance beyond the point where that glaciation of which evidence has so far been fonnd in river leaves the mountains but where it is still bordered Alaska. by foothills. High ridges of Tertiary gravel, standing Unpublished manuscript notes by Eliot Bla^kwel- 12,600 feet above the level of the Nenana River, con der refer to a body of tillite, containing polished and tain on their surface numerous large boulders and scratched pebbles, on the Yukon Biver near Wood- erratic blocks that many geologists agree are of glacial chopper Creek and to an imbedded clay slate, studded origin. These boulders are found as far as 25 miles with chunks and pebbles of other rock, on P*iaver north of the recognized moraines of Wisconsin age and i Caimes, D. B., The Yukon-Alaska International boundary, between Porcupine and Yukon Rivers: Canada Geol. Survey Mem. 67, pp. 91-83,1914. • Capps, S. B., The Chisana-White Kiver district, Alaska: U. S. Geol. Survey * Mertie, T. B. Jr., Geology of the Eagle-Circle district, Alaska: tr. 8. Qeil. Survey £ull. 630, pp. 63-69,1916. Bull. 816, pp. 24-28, 1930. 8 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 Creek. He thought that both these occurrences River Basin, at a locality that Res close to tin terminus represented glacial deposits and tentatively guessed of an active glacier and therefore does not prove an ice their age to be Cambrian. Mertie, 9 thinks that the expansion much beyond that of present glaciers; of first of these formations is of Devonian age and the glacial boulders in the Nenana Valley that lie many other late Silurian, and he doubts the validity of miles north of the limit reached there by Wisconsin Blackwelder's conclusion as to their glacial origin. glaciers; and of an old till in the Mulchatna Basin that Kirk 10 describes a Silurian conglomerate occupying was deeply oxidized before the Wisconsin advance but a considerable area on Prince of Wales Island and that lies well back within the area covered1 by ice in neighboring islands in southeastern Alaska which has Wisconsin time. locally a thickness of 1,000 to 1,500 feet and in which CONCLUSION he found abundant faceted and striated boulders. He It is probable that in Alaska, as in other parts of the entertained no doubt that this is a glacial deposit. world, there have been recurrent glacial periods from Kirk further describes faceted pebbles in a limestone mid-Paleozoic time to the present. This was to have of Middle Devonian age on Prince of Wales Island and been expected, for unless the earth's poles have wan rounded boulders in Lower or Middle Devonian sedi dered much farther than has been determined, the ments near the north end of Chichagof Island, to high latitude of Alaska would always ha^e favored which he doubtfully attributes a glacial origin. glaciation there as compared with more temperate At still other localities in southeastern Alaska, as at lands. Furthermore, for much of geologic time there Pybus Bay, on Admiralty Island, and on the Screen have probably been high mountain areas in Alaska, Islands, off the west shore of Etolin Island, Kirk found and in these areas local glaciers might have been faceted but no striated pebbles in beds of Permian fostered even when glaciers couM not esist in the age that he thinks may be glacial. lowlands. Blackwelder n considers certain conglomerates of Pleistocene glaciation in Alaska was severe, prob the Yakutat series, in the mountains east of Yakutat ably during several stages but certainly during Wis Bay, to be glacial deposits, and the boulders in asso consin time. The surprising fact is that so large an ciated shales to have been dropped by icebergs. These area in subarctic and arctic Alaska should have re rocks, according to Blackwelder, have been assigned mained unglaciated while the remainder of northern to the Jurassic by Ulrich, though C. W. Wright thought North America was submerged beneath successive they were probably of late Carboniferous age. continental ice sheets. The restriction of Pleistocene It will thus be seen that the evidence of pre-Pleisto- glaciation in Alaska to mountainous area-* was due cene glaciation hi Alaska includes a questionable mainly to a semiarid climate in the lower country. tillite of Cambrian age near the international boundary If the climate of to-day may be considered to be as in Yukon Basin; one fairly well established occurrence mild as the average climate during the several Pleisto of tillite in the Silurian of southeastern Alaska, and a cene interglamal stoge®, then there is every likelihood less certain one in the late Silurian of the Yukon that mountain gjaeififs aw© survived conti*MiQWsly in Basin; questionable occurrences of Devonian age in the higher mountains of Alaska from the beginning of the Yukon region and in southeastern Alaska; a doubt Pleistocene time to tlfc© present and that the Pleisto ful occurrence of glacial material near Yakutat that cene ice advances were merely expansion and the may be of Carboniferous or of Jurassic age; and a interglacial stages contractions of eontinnc^isly exist possible glacial deposit of Permian age in southeastern ing glaciers. In other words, in Alaska glaniation has Alaska. been continuous since the beginning of the Pleistocene To summarize the evidences of glaciation in Pleisto epoch. • cene time before the Wisconsin stage, we now know of If the concisions set forth above are justified, it tillite, indurated and uplifted to a height of 5,000 feet follows that the present time of restricted glaciation is above sea level, on the south flank of the St. Elias possibly only an interglaeial stage. The time that has Mountains, but occurring in the midst of great present- elapsed sine© the Wisconsin ice invasion i*> probably day glaciers and so having no certain correlation with shorter than half the average duration of the Pleisto early great ice transgression; of an uplifted and tilted cene interglacial stages. Whether or not the maxi succession of tillite, gravel, and silt beds in the White mum stage of deglaciation has been reached is not known, but it is entirely possible that sometime within • Mertie, J. B., jr., oral communication. w Kirk, Edwin, Paleozoic glaciation in southeastern Alaska: Am. Jour. Sci., 4th the next 50,000 or 100,000 years or so the northern ser., vol. 46, pp. 511-515, 1918. part of the continent may again be subjected to sub « Blackwelder, Eliot, The probable glacial origin of certain folded slates in south eastern Alaska: Jour. Geology, vol. 15, pp. 11-14,1907. mergence beneath a continental ice sheet, THE UPPER CRETACEOUS AMMONITE GENUS BARROISICERAS IN THE UNITED STATES By JOHN B. REESIDE, Jr. INTRODUCTION The name was printed in the original text as Bar- The ammonite genus Barroisiceras Grossouvre is roisia, but as this name had been applied to a genus noteworthy because of its wide geographic distribution of sponges in 1882 by Munier-Chalnias, Grossoi'vr© in and its apparently small stratigraphic range. It is an added note altered the form of his new tr«?in to reported from deposits of Coniacian age in Europe, Barroisiceras. Grossouvre's characterization of the Africa, South America, and North America. In the genus consisted chiefly of a comparison of the suture North American Upper Cretaceous it is rather rare, with that of Tissotia DouvilMj, in whicsh. it was stated authentic species having been recognized hitherto that Barrouieeras differed in having fewer lobes, only in the Austin chalk of Texas, in the Coniacian greater incision of the element®; and the larger member beds of Zumpango del Rio, Guerrero, Mexico, and, of the unsymmetrically bifid external saddle on the with doubt as to the source, in. New Jersey. The siphonal side. Grossoiivre's figures and diseasjmon of Texan species, B. deniatocarinatum (Roemer), is by no the species afforded other characters, however, useful means an abundant form, though among those de for recognition of tibe genus. The species h&bwf*Uneri scribed in early work in the region. The Mexican was given a very wide scope and included besicSs the representatives of the genus thus far described include typical form the varieties al^tademnsis Schlute^,3 cfes- only fragmentary specimens not specifically named. moulinsi Grossouvre, and harlei Grossouvf©. The The occurrence ascribed to New Jersey is based on a other species recognized were B. nwkUsi Grosawrre, fragment that seems to belong to Barroisiceras but B. sequens Grossouvre, and B, boisselleri Giesrmvre. whose source is very doubtful. Under B. haberfellneri Grosgmrrae included — fa addi The present paper records, in addition to B. dentato- tion to Schliiter's Ammonites (d$tadenenm»— A. carinatum, five new species from the Interior Province coriensis Coquand,4 A. nepfami Fritsefa., and £ i and one from Texas. Five of these are represented by bach (not Geinite),5 A. dentaJo-carinoMts •Fritsrh .and single specimens and one by two specimens, but all Schlonbach. (not Roemer),8 A. pmon Redteab^aer,7 are well characterized and deserving of recognition in and Buehiceras nardini Fallot.8 Grossouvre suggested spite of scant material. Three of the new species are also that Schloenbachia tunetana Peron * may be a associated with other invertebrates of early Niobrara Barroisiceras but stated that !he did not know any (early Coniacian) age and come from one locality in Indian or American species. the Mancos shale of central Utah. A fourth is like Peron 10 in 1897 noted B. haberfeUmri Gros^mvr© wise associated with invertebrates of Niobrara age in Algeria, doubting, however, the validity of Stating and comes from the Frontier sandstone near Lander, with it Ammonites petrocoriensu Coquand. Wyo. The fifth new species is from the Timpas lime Anderson " in 1902 included Barroisieeras in S-'Mom*- stone, the lower formation of Niobrara age, near Car- bachia, referring to it two species, S. lile Springs, Colo. The sixth is from the Austin 3 Schlflter, Clemens, Cephalopoden der oberen deufcscheo Kreide: chalk north of Sabinal, Tex. phica, Band 24, p. 151, pi. 40, figs. 1&-16, 1876. 4 Coquand, Henri, Synopsis des animaux et des vegfitaux fossites obser? 4» daas la Mr. W. O. Hazard photographed the specimens formation crgtacee du sud-ouest de la France: BOG. gfoL Prance Bull., 3d se-., vol. 16, shown in the plates, and Miss Frances Wieser re p. 995, 1868. ' Fritsch, Anton, and Schlonbach, Urban, Cepbatopoden der biiflmiscben Kreide- touched the photographs and assembled the plates. formation, p. 30, pi. 15, fig. 3, Prague, 1872. « Idem, p. 32, pi. 16, figs. 1-3. TAXONOMIC HISTORY OF THE GENUS BARROISICERAS ? Redtenbacher, Anton, Die Ceplialopodenfauna der Gosauaeflichtea in den nordostlichen Alpen: K.-k. geol. Reichsantsalt Abb., Band 5, p. 103, pi, 23, fig. 3, GROSSOUVRE 1875. 8 Fallot, J. E.T Etude geologique gar to Stages moyens et superieurs du terrain The genus Barroisiceras was instituted by cretac6 dans le sud-esfc de la France: Annales fid. geol., vol. 18, p. 241, pi. 3, figs. Grossouvre * in 1894, with Ammonites haberfellneri 3-4, 1866. 8 Peron, Alphonse, Description des invertSbrfe fossHes des terrains ere'ticfe de la Hauer 2 as the first species and chief basis of the genus. region sud des hauts-plateaus de la Tunisie reeoeillis en 18S6 et 1886 par M . Philippe Thomas, pp. 21-23, pi. 17, figs. 6-8, 1893. 1 Grossouvre, Albert de, Les ammonites de la Craie supfirieure: Carte gSol. France i» Peron, Alpbonse, Les ammonites da Cr$£ae$ supfirieur d« TAlgfirfe: Soe. gW. M6m., Recherehes snr la Craie supfirienre, pt. 2, Paleontologie, pp. 80-81,1893 [1894]. France M6m. 17, p. 48, 1897. 2 Hauer, Franz von, Neue Cephalopoden aus den Gosaugebilden der Alpen: n Anderson, F. M., Cretaceous deposits of the Pacific coast: California Aead. Sei. K. Akad. Wiss. Wien SiUungsber., Band 53, Abt. 1, p. 301, pi. 1, figs. 1-6,1866. Proc., 3d seaf., voL 2, no. 1, pp. 119-120, 1908. 0 10 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 Anderson and S. (J5.) knighteni Anderson, from the umbilicus aad forked rite, and to Cfetif&fe*te«r«ts, but lower part of the Chico formation of Oregon and separable by its lesser involution, shallow fam>ws California. It is difficult to judge Anderson's figures bordering the median keel, and the sharp decrease and descriptions, but the assignment to Barroisiceras inward in the heigh* of the stitural elemerts. Solger seems doubtful because of the sigmoid curvature of raised the variety *&sflW«K?m GiwsoufTe to specific the ribs, weak marginal tubercles, and other features. rank because specimens from Africa stud"*d by him It is also highly probable that the lower Chico is and assigned to it possess a smooth keel at all stages, older than any beds containing true Barroisiceras. and he described the new species B. &ra»d*n, dividing Hyatt 12 in 1900 in a general arrangement of the it into the two varieties mitis and armata. Ammonoidea assigned Barroisiceras to the family Lasswitz 16 in 1904 assigned to ScUoenb^chia (Bar Mammitidae, giving only a brief discussion of the roisiceras) a number of species from Texas, supposing family. He included with Barroisiceras and Mammites them to be of Coniacian age. They have since been his new genera Calycoceras and Metacanthoplites, the found to be much older and recently have been placed latter based on Ammonites rhotomagensis Defrance, by Bose 17 for the greater part in his genus Budaiceras. now generally accepted as the genotype of Acan- Only the species fanta&ocarinatnm Koemer 1S appears thoceras. to be an authentic Barr&meer&s. Hyatt 13 in 1903 interpreted the genus, apparently Pervinquiere 19 in 1§07 accepted Solger's diagnosis on the basis of Grossouvre's published data only, as of the genus; added a new species, B. romieuxi, and a possessing smooth, compressed young with continuous new variety, byzacenicum, of B. haberfellneri; and, keel; successive later stages with ribs and a smooth following Grossouvre's suggestion, assigned to the keel; with ribs, nodes, and a nodose keel; finally with genus ScMoenbachia tunetana Thomas and Peron with a smooth keel again. He considered the several varie a new variety, inerme, under it. He listed as species ties of B. haberfellneri to be distinct species and named of Barroisiceras B. haberfellneri (Von Hauer), with one of Grossouvre's figured but unnamed variants of varieties alstadenense (Schliiter), harlei Grossouvre, this species B. haueri. and byzacenicum Pervinquiere; B. nicklesi Grossouvre; Shattuck 14 in 1903 referred to Barroisiceras two B. desmoulinsi Grossouvre; B. tunetanum (Thomas and species from the Buda limestone of Texas as B. texanum Peron), with variety inerme Pervinquiere; B. seguens Shattuck and B. hyatti Shattuck. The horizon of Grossouvre; B. boissetteri Grossouvre; B. brancoi Sol these forms is considerably below that of other species ger, with varieties mite Solger and armafum Solger; included in the genus, and both have since been placed and B. romieuxi Pervinquiere. He rejected B. texanum in Budaiceras Bose, as noted below. Shattuck and B. hyatti Shattuck as doubtful, a pro Solger 15 in 1904, in a discussion of fossils from cedure justified by their later inclusion in Budaiceras. Kamerun, gave the first real description of Barroisi He did not note B. haueri Hyatt and ignored the forms ceras, which may be translated as follows: cited by Lasswitz fwnj Texas. Shell high-whorled and with rather narrow umbilicus except Welier 20 in 190? *e%ia»€l and described m B&rrom* in the old-age stages of soine forms. Periphery with a smooth cerm 4mt@M&«mfv®a$m Mciemer a fragment of a whorl or nodose keel accompanied on either side by a row of nodes or of an ammonite which'WMtield*1 had earMer figured a smooth slope. as AmmmJimf jkiSfatf&*&ti,nQt'a#. The s^eennen is Flanks smooth or bearing rounded ribs, sometimes also hardly-JBL I. Median-ventral nodes equal in number to the marginal nodes. I. Median-ventral nodes equal 3ta number to the ma-*a^naliiodes; 1. Ribs straight—Continued. 1. Ribs straight—G^ntta«ed. A. Strong umbilical and marginal nodes—Continued. B. Median-lateral as well as umbilical and marginal a. Bibs well developed—Continued. nodes* neptuni (Fritsch and Schlonbach) (not c. Ribs distinct; median-lateral nodes not stronger Geinitz). Fritsch and Schlonbach, p. 30, than others; shell relatively compressed. pi. 14, fig. 3, 1872. Much like haberfell- sfefo^HNmwt (SeMttter). SeMuf«r, p. 151, neri but with weaker sculpture. Umbilicus pi. 40, figs. 13-16, 1876; Grossouvre, p. 51, one-sixth diameter. pi. 1, fig. 4, pi. 2, fig. 4, 1894. In earlier dentatocarinatum (Fritsch and Schlonbach) stages 7 umbilical and median-lateral nodes (not Roemer). Fritsch and Schlonbach, and 21 ventral nodes per wl^ii; in later p. 32, pi. 16, figs. 1-3, 1872. Rather com stages ribs and nodes disai i-jear except pressed, ribs on flanks weaker than in marginal nodes., Umbilicus one-sixth di haberfellneri; nodes about same number as ameter. in haberfettneri, but umbilical nodes accen olstadenense Solger (not Schliiter). Solger, tuated. Umbilicus one-fourth diameter. p. 170, pi. 5, fig. 6, 1904. Umbilical and paeon (Redtenbacher). Redtenbacher, p. median-lateral nodes weak, marginal and 103, pi. 23, fig. 3, 1875. Rather com median-ventral nodes strong; ribs persist pressed; in earlier whorls 9 umbilical nodes longer than in alstaden&me s. s.; only 2 and 24 ventral nodes; in later whorls marginal nodes for each umbilical node. ventral nodes unite in a high, smooth keel Umbilicus one-fifth diameter. and marginal nodes weaken. Umbilicus sevierense Reeside. This paper, p. 16, pi. 4, one-eighth diameter. figs. 4-8. Nodes and ribs moderately 6. Ribs weak. strong; 10 umbilical and ncedian-lateral dentatocarinatum (Roemer). Roemer, p. 33, nodes, 16 marginal and median-ventral pi. 1, fig. 2, 1852. Shell much compressed; nodes per whorl, aE persistent. Umbilicus ventral nodes high and sharp; 5 umbilical, one-fifth diameter. 25 ventral nodes per whorl; in large adults 6. Ribs very weak; median-lateral nodes prom the marginal nodes pass into distant blunt inent; shell relatively stout. spines. Umbilicus one-fourth diameter. forresteri Reeside. This paper, p. 17, pi. 5, petrocoriense (Coquand). Grossouvre, p. 51, figs. 2-7. Blunt spinelike iredian-lateral pi. 2, fig. 5, 1894. In early stages ribs and and r0af|£Uial nodes, weak umbilical and nodes distinct, 8 umbilical and 18 ventral median-ventral nodes; 12 umbilical and nodes per whorl; in later stages ribs median-lateral nodes, 18 irnrgmal and and umbilical nodes vanish. Umbilicus median-ventral nodes per whorl. Umbili one-sixth diameter. cus one-fourth diameter. dartoni Reeside. This paper, p. 16, pi. 6, allaudi (Boule, Lemoine, and Thevenin). figs. 8-10; pi. 5, figs. 8-9. Shell com Boule, Lemoine, and Thevenir, p. 32, pi. 8, pressed, cross section of whorl high oval; figs. 6-7; text fig. 17, 1907. Blunt spine- 11 umbilical, 20 marginal and ventral like median-lateral and maa'fdnal nodes, nodes per whorl, persisting to end of shell. weak umbilical and median-ventral nodes; Umbilicus two-sevenths diameter. • 15 umteiMcal and median-lateral nodes, 23 nicklesi Grossouvre. Grossouvre, p. 63, pi. 3, - -. marginal sod median-ventrsl nodes per fig. 2, 1894. Shell much compressed; 8 Uaotbfliciis one-fourth diameter. coarse umbilical and 20 ventral nodes per * Reedde. This paper, p. 17, pi. 7, whorl; ribs obscure; keel faiat and scarcely 1-7; pi. 6, figs. 1-3; pi. 7, fig. 1. In tuberculate in later stages. Mature cross early stages median-lateral noies not much section subquadrate. Umbilicus one- moss pcoaainent than the otl *ws; in later fourth diameter. stages umbilical and median-lateral nodes nicklesi Boule, Lemoine, and Thevenin (not »re Jotaedi by high rib and bee«pae eoospie- Grossouvre). Boule, Lemoine, and Theve uous; all the nodes persistent. Umbilicus nin, p. 45, pi. 11, fig. 2, 1907. Shell stouter one-tbiid diameter. than in nicklesi s. s., umbilicus smaller hobsoni Reeside. This paper, p. 18, pi. 9, and umbilical nodes weaker; median- figg. *2~4j pi. 8, figs. 1-2. In early stages ventral nodes persist to a larger stage. mmbiBmt. nodes fairly steonr, others of Umbilicus one-fifth diameter. sanae siae; In later stages uirbilical nodes nttrdini (Fallot). Fallot, p. 241, pi. 3, figs. disappear, each third median-lateral node 3-4, 1885. Shell compressed; 8 coarse becomes a strong blunt spine, and the Umbilical and 16 marginal nodes per whorl; mecBan-veatral nodes weaken somewhat. former on sharp umbilical shoulder; ribs Umbilicus one-third diameter. weak in early stages and absent in middle and later stages. Mature cross section subquadrate. Umbilicus one-fifth diameter. THE UPPER CEETACEOUS GENUS BARROISICEBAS I. Median-ventral nodes equal in number to the marginal nodes. I. Median-ventral nodes equal in number to the marginM aod«s. 1. Ribs straight—Continued. 2v Ribs sigmofci—Continued. f ,r C. Sculpture very weak; ribs weak or absent; marginal B. Keel smooth; ribs weak. nodes strongest, median-ventral nest, seqwm Grossouvre. Grossouvre, pCfti, pi. 8, umbilical nodes weak or absent. Shell fig. 1, 189*. Ribs broad, pers&fr^;ia^o compressed. late stages; marginal nodes pc^Hi^kt. a. Small species with small umbilicus and sharp- Umbilicus one-fourth diameter. ventered adults. b&issdleti Grossouvre. Grossouvfe, p, fl§, harlei Grossouvre. Grossouvre, p. 51, pi. 2, pi. 3, fig. 3,1894. Ribs narrow, ]j«i*fe!tca& figs. 2, 7, 8, 1894; Boule, Lemoine, and fewer than in sequens; tnargtaa 1 , nodes Thevenin, p. 43, pi. 11, fig. 4, 1907. In - persistent. Umbilicus one-third are much more alike than the later stages. The ense, B. dartoni, B. nwkfam (Orossotrrre), B. nicklesi mature B. haberfellneri, for example, has a rather (Boule, Lemoine, and Thevenin), and B. nardini. broad and concave venter, B. paeon has a smooth per For this subgeneric group the name Texa^w is here sistent high keel, B. harlei has an obtusely angulate proposed. venter, and B. brancoi has a rounded venter, though The group of Banr&uwems GtstademneG contains the earlier stages have many features in common. small to medium-sized species, probably no* exceeding^ Some adults develop strong sculpture, others are nearly 100 millimeters in diameter. The cross section of the smooth. Some are much compressed shells, some are whorl is high and moderately compressed. The relatively stout. umbilicus is of medium size, one-fifth or ors-sixth the All species of Barroisiceras have, at least in the early diameter. The ribs are fairly steong and ornamented and middle stages, three rows of subequal nodes on the by a median-lateral row of nodes as well ar umbilical, venter—one on the median line and one on each mar marginal, and median-ventral nodes. Hem belong B. gin, forming a more or less sharply defined ventro- alstadenense (Schliiter), B. alstadenense (Solger), and B. lateral shoulder. Each median node is set forward of sevierense. For this subgeneric group the name its corresponding pair of marginal nodes. Most spe Alstadenites is proposed. cies have also a row of nodes on the umbilical shoulder The group of Barroisiceras Jorresteri contains species and some a row on the middle of the flank. The ribs that attain a large size, as much as 200 niillimeters in are invariably straight, directed radially, and increase diameter. The cross section, of the whorl is stout, both by forking and intercalation. The suture is subquadrate. The umbilicus is relatively large, one- moderately dissected, has three or four rounded lateral third or one-fourth the diameter. The ribs are weak, saddles, all high, and a first lateral lobe as long as or but the umbilical, median-lateral, marginal, and longer than the siphonal lobe. The other lobes are median-ventral nodes are strong, the median-lateral small. nodes in the later stages of some specier becoming1 The six groups may be conveniently looked upon as blunt spines. Here belong B.forresteri, B. attaudi, B. subgenera, though doubtless some of the present-day stantoni, and B. hobsoni. For this subgeneric group students of ammonites would consider several of them the name Forresteria is proposed. genera. The group of Barroisiceras harlei contains small to The typical group, that of Barroisiceras haberfell medium-sized species, not much exceeding; 100 milli neri (Hauer), contains small to medium-sized species, meters in diameter. The cross section of the whorl is. usually not much more than 100 millimeters in diam high and much compressed. The umbilicus is small, eter. The cross section of the whorl is high and one-eighth the diameter. The sculpture is very weak; moderately compressed. The umbilicus is small, one- ribs weak or absent, marginal nodes only moderately fifth to one-eighth the diameter. The ribs are fairly strong, median-ventral weak, umbilical w^ak or ab strong and are ornamented by strong umbilical and sent. In late stages the siiell is nearly sarooth, with, marginal nodes. Large adults differ much. In B> venter obtusely angulate. Here belong B. harlei, B. haberfellneri the median-ventral nodes fade out, but bysaeemcum, and B, castettense. For this subgeneric the marginal nodes remain and the venter is broad and group the nanae Horfotfes is proposed. concave; in B. paeon the median nodes fuse into a high The group of Bmroiswems braneoi SolgiT contains smooth keel, but the marginal nodes weaken; in both fairly large shells, as much, as 200 millimeters in species the ribs weaken greatly. Here belong B. diameter. The esross section is high and much com haberfellneri, B. haueri, B. neptuni (Fritsch and pressed. The mnbiHcwE is relatively large, one-fourth Schlonbach), B. dentatocarinaium (Fritsch and Schlon- or one-fifth the diameter. The sculpture is very weak; bach), and B. paeon. This group is, of course, ribs weak, the marginal and median-ventral nodes Barroisiceras s. s. somewhat stronger, umbilical nodes verrr weak or The group of Barroisiceras (kntatocarinatwm, (Boe- absent, in adults tae median-ventral nodes dis mer) contains species that may reach a relatively appear and tibe veatet is rounded. Here belong B. large size, as much as 200 niillimeters in diameter. braneoi var. mite and B. r&mtiewci. B. branem var. ®nm- The cross section of the earlier whorls is subtriangular, tum develops large, distant, blunt spines but otherwise of the later whorls high and much compressed, sub- agrees and may be tentatively included. For this quadrate in most forms, oval in others. The umbili subgeneric group the name Stolg&rites is hen? proposed. cus is relatively large, one-fourth or one-fifth the diam Barroisiceras is superficially much like ceHain forms eter. The ribs are weak in the early stages and dis assigned to Prion&tropi® Meek of the Turanian. It appear later, but the umbilical and marginal nodes has been much debated, for example, whether to remain strong and persistent. The median-ventral admit Ammonites jfawiwiManus D'Orbrmy81 into nodes remain throughout, becoming a faintly nodose » D'Orbigny, Alcide, Pal6ontologie franeaise, Terrain cr6tae6, O£phalopodes, p. keel. Here belong B. dentatocarinatum, B. petrocori- 350, pi. 107, 1841. ' THE ITPPEB CBETACEOTTS GENUS BAKBOISICBSAS Barroisiceras, but it would seem better placed in This beautiful species, escelleatly charaeteriBed by its Prionotropis, though, certainly not typical. Priono- discoid form and its keel of distant, compressed teeth, is differ^ ent from all other known species. * * * tropis has simple ribs inclined forward on the flanks Occurrence: Waterfall of the Guadalupe near New Err and bent sharply forward on the venter, of unequal (Translated from Roenaer, 1852.) prominence in the early stages, more nearly equal in The great compwession of the whorls, at a the later stage. There are no umbilical nodes, but part secondary, of all the available double marginal nodes; and the ventral nodes in figures of this species makes comparisons of form early stages form a true, individualized keel. The difficult. It was very likely a much compressed r^eeies umbilicus is relatively large. Several other genera at all stages, however, even before fossiJjjsation. In also have been brought into comparison by authors. sculpture its weak ribs from a diameter of 20 milli Gauthiericeras Grossouvre is separable by its con meters to that of 150 millimeters and the development tinuous keel at all stages, simple ribs, and wide um of blunt spines in the very large stages separ%te it bilicus. Tissotia DouvU16 is easily separated by the from most other species with only margin* 1 and suture, particularly by the entire saddles, and the umbilical nodes. From B. petroeonense Coquari n it continuous keel. Heterotissotia Peron has a truncated differs in the earlier stages in its weaker ribs, larger venter and lacks the median-ventral nodes. Pseudo- umbilicus, and higher, coarser keel. tissotia Peron has a continuous keel and very small One of the specimens here figured, an, internal mold umbilicus and differs in sutural detail. collected by L. W. Stephenson, is from the typ« local ity. It is smaller than the type and differs, if Roger's NORTH AMERICAN SPECIES OF BARROISICERAS figure and description are accurate, in that the median- Barroisiceras (Texasia) dentatocarinatum (Roemer) Lasswitz ventral nodes are not opposite those of the nr^rgins of the venter, but each lies somewhat forward of the Plate 3, Figures 1-10; Plate 4, Figures 1-3; Plate 5, Figure 1 corresponding marginal nodes, as in other spe?ies of 1849. Ammonites dentato-carinatus Roemer, Texas, p. 417. Barroisiceras. Possibly the original description k 1852. Ammonites dentato-carinatus Roemer, Die Kreidebildun- faulty in this detail, but only the type its€*f can gen von Texas, p. 33, pi. 1, figs. 2a, b, c. settle the matter. The umbilicus is a trifle wid°ir and 1904. Schloenbachia (Barroisiceras) dentato-carinata (Roemer). Lasswitz, Paleont. Abh., n. F., vol. 6, p. 249. the ribs and nodes somewhat fewer—2Q as agafrist 24 1926. Barroisiceras kaberfellneri (Hauer) (part). Scott, Gre noted by Roemer. noble Univ. Annales, new ser., sci. sec., vol. 3, p. 109. A large internal mold, probably representfflf a nearly 1928. Barroisiceras dentatocarinatum (Roemer). Adkins, Texas complete shell and associated with Inoeemmm aff. J, Univ. BuU. 2838, p. 252. deformis Meek, was collected by N. H. Darto^ at a Not 1872. Ammonites dentato-carinatus Roemer. Fritsch and locality north of Hondo, Tex. The earliest whorls Schlonbach, Cephalopoden der bohmischen Kreide- formation, p. 32, pi. 16, figs. 1-3. exposed, at a diameter of 80 miUiaieters, am at a Not 1892. Ammonites dentato-carinatus Roemer. Whitfield, larger stage than the type or the other specimens in U. S. Geol. Survey Mon. 18, p. 250, pi. 41, figs. 3-4. hand but agree sufficiently well with them to warrant Not 1907. Barroisiceras dentato-carinatus (Roemer). Weller, the assignment of the specimen to B, dmb^-mrm®* New Jersey Geol. Survey Paleont. Ser., vol. 4, p. 836, turn. The later stages present features of consider pi. 101, figs. 5-6. able interest. The cross section of the whorl i-» high, Diameter of shell, 3 inches (75 millimeters); height of last subrectangular. The sculpture continues witls little whorl, 1 inch 5 lines (35 millimeters); height of next to last whorl, 8 lines (17 millimeters). change to the stage at a diameter of 150 BaltBneters. Shell discoid, compressed, umbilicate, keeled on the back There the marginal nodes, instead of remamiig sub- (venter), ornamented on the flanks with nodes and poorly de equal, begin to differ in size, each third one on the fined ribs. The whorls increasing rapidly in height, slowly in remainder of the shell becoming a prominent blunt width, two-thirds covered. The flanks flat, almost parallel. spine, whereas the intervening nodes become ©Yea The keel is interrupted and consists of large sharp-edged com pressed teeth with rounded points. The back (venter) is bor smaller than those on the earner parts of the shell. dered on either side by a row of nodes, which stand opposite the A little more than the last half whori of this sp-^eimen teeth of the keel and are 24 per whorl in number. From each of is unseptate, the maximum diameter being 210 milli- these nodes a weak fold runs toward the umbilicus. The most meters. The aperture is not preserved. of these disappear, however, on the middle of the flank or Another internal mold of part of a whorl, ec^teetecl beyond it. Only a few folds, indeed each third or fourth, reach by T. W. Stanton at a. locality in the Bio Orande the umbilicus and end in a blunt node standing on the edge of the steeply descending umbilical wall. Six such nodes are present Valley, agrees well with the species. on each side of a whorl. The lobes of the septum are strongly dis Formation and localities: Austin chalk at tH falls sected and branched. Individual branches of the lobes are very of the Guadalupe River, 2 miles below the brid*^ east slender and run out into pointed ends. The dorsal (ventral) of New Braunfels, Comal County, Tex,; Cbw Greek lobe almost as deep as the first lateral lobe; the second lateral below Pinto Creek, about 24 miles below J>4 Bio, lobe much less deep and narrower than the first. In addition an oblique-lying small auxiliary lobe. » Grossonvre, Albert d«, op. dt., p. 51, pi. 2, flg. 5. 62508°—32——2 16 SHOKTEK CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 Tex.; Verde Creek, 8 miles north of Hondo, Medina Formation and locality: Austin chalk near the County, Tex. Sabinal-Utopia road, 5 miles north of Sabraal, Uvalde County, Tex., associated with Inocerawus aff. J. Barroisiceras (Texasia) dartoni Reeside, n. sp. deformis Meek and Qryphaea aff. Q. aucella Roemer. Plate 6, Figures 8-10; Plate 7, Figures 8-9 One internal mold, somewhat compressed and not Barroisiceras (Alstadenites) sevierense ReesHe, n. sp. showing the sutures, is the basis of this species. Plate 4, Figures 4-8 Probably the last three-fifths of a whorl represents the living chamber, as the preceding part of the shell One entirely septate internal mold shoeing a full is much more compressed. The maximum diameter whorl and the umbilical part of the preceding whorl is preserved is 145 millimeters; the earliest "stage show the basis of this species. Maximum dirmeter pre ing the venter, a volution earlier, is about 70 milli served is 60 millimeters; earliest stage showing the meters in diameter, though the flanks of the next venter is at 25 millimeters diameter. preceding whorl, to a diameter of perhaps 25 milli Shell a moderately stout disk. Very e Solger \not Schliiter) M it differs in its more persistent in the type the umbilical nodes are still weak, and coarser sculpture, having scarcely two-thirds as very weak, but th© median lateral nodes have many ribs and nodes. blunt spines; the marginal modes are still The specific name is derived from Sevier County, the median-ventral nodes are relatively weaker. Utah, where the specimen was found by the .late The suture shows the siphonal and first lateral lobe® Robert Forrester, o£ Salt Lake City, Utah. subequal in length, the second lateral lobe skor% wad Formation and locality: Mancos shale, 200 feet the third very small; the first lateral saddle a little above the Ferron sandstone member, at a locality in wider than the siphonal lotfe; the first latera1 lobe Sevier County, Utah, 4 miles east of Oak Spring and rounded-trifid, the second lateral lobe almost c*r the about 12 miles west of south of Emery. In the same umbilical shoulder. beds were Barroisiceras jorresteri, B. castellense; Barroisiceras' Jorresteri is characterized by its stout species as yet unnamed of Scaphites, Bacidites, Placen- shell and strong sculpture, particularly the de^elop- ticeras, "Helicoceras," and Euirephoceras; Inoceramus ment of the median-lateral and marginal node' into deformis Meek, and other pelecypods. At near-by blunt spines. The writer knows no close American localities the upper part of the Ferron sandstone relatives. B. desmovlinsi Grossouvre85 has the g^tieral member contains Prionocyclus wyomingensis Meek, aspect of B.- forresteri but lacks the median-lateral P. macombi Meek, Prionotropis hyatti Stanton, Sca nodes and is said to have a smooth, continuous Ireel at phites warreni Meek and Hayden, Ostrea lugubris all stages.86 Conrad, and Inoceramus fragilis Hall and Meek. B. Jorresteri seems very close indeed to the form Barroisiceras (Forresteria) forresteri Reeside, n. sp. from the Senonian of Diego-Suaxez, Madagascar, described by Boule, Lemoine, and Thevenin 87 as Plate 5, Figures 2-7 Acanthoceras (Prionotropis) attmidi^ which seenas to One entirely septate internal mold showing parts the writer to be a species of Baar&mc&fw. B./0r*^sfen of two whorls is the basis of this species. The entire differs chiefly in its fewer ribs and nodes. whorl from a diameter of 13 mfllimp.tp.ra to that of 28 The species is named for the late Robert Forrester, millimeters is present, though only about half of it is of Salt Lake City, Utah, who collected tike type. completely exposed; and the half whorl from a diam Formation and locality: Same as for eter of 42 millimeters to that of 55 millimeters is preserved. Barroisiceras (Forresteria) sianioai Reeside, n. Sf Shell a very stout, spinose ovoid. At a diameter of Plate 7, Figures 1-7; Plate S, Figures l~g; Plat© $, 14 millimeters the width of the whorl is three-fourths the height (4.5 by 6 millimeters) but gradually This species is based on two internal molds from changes until at the diameter of 28 millimeters the the same locality — a laJfger one, chosen, as the type* whorl is as wide as high, excluding the nodes, and one- with a maximum, diameter of 130 millimeters, and a fifth wider than high, including the nodes (16 by 13 smaller one, with a maximum diameter of 39 milli millimeters). At about 50 millimeters diameter the meters. The part of the shell at less than 50 rniUi* whorl is 25 millimeters high and 25 millimeters wide, meters diameter shows only in the umbilicus of the excluding the nodes, and 33 millimeters wide across larger specimen, and that below 14 millimeterf only the nodes. The general aspect of the later cross- in the umbilicus of the smaller specimen. section is depressed hexagonal. Umbilicus between Shell a thick disk, of medium size for the jrenus. one-third and one-fourth the diameter; umbilical Cross section roughly hexagonal from a diftmetei of 14 shoulder fairly distinct and somewhat rounded; um millimeters to 80 millimeters (aJjout the position of the bilical wall steep. Living chamber and, aperture un last septum of the type), being relatively high ia the known. early stages and much, more depressed and I *oad- Sculpture from 14 millimeters diameter to 20 milli ventered in the later stages; cross section of the living meters diameter, a half whorl, shows no umbilical chamber subquadrate. Umbilicus 40 miffimeterr wide nodes; 6 rounded primary ribs which end in conical at the end of the type, a little less than one*4hiHl the median-lateral nodes and there mostly divide into diameter, but in the earlier stages it is proportion mtdiy secondary ribs, which in turn, end in conical marginal smaller, being a little more than one-fifth, the diameter nodes 10 in mumber; median-ventral nodes, each at 39 millimeters. Umbilical shoulders abrupt at all placed somewhat forward of the corresponding mar stages seen, with inner wall nearly at right angles to ginal nodes. On the succeeding half whorl, to 28 the flank. laving chamber of type occupies tnree- millimeters diameter, weak umbilical nodes appear f ourths of last whorl, aperture unknown. and the median-lateral and marginal nodes increase in a« Grossouvre, Albert de, op. clt., p. 61, pi. 2, %. 6. , relative strength. On the final half whorl preserved M Solger, Frledrich, op. cit., p. 167. 8? Boule, Marcellin, Lemoine, Paul, and Theveain, Annaad, op. cit., p. 32, p}. 8, * Solger, Friediich, op. cit., p. 170, pi. 5, %. 6. figs. 6-7, text flg. 17. 18 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 Sculpture at the diameter of 10 millimeters shown The species is named for Dr. T. W. S+anton, who only in the umbilicus of the smaller specimen, where collected the type and paratype. there are rather coarse primary ribs without well- Formation and locality: A sandstone in T. 33 N,, defined umbilical nodes; any other nodes that may be K. 99 W., southeast of Lander, Wyo., inchided in tHe present are covered by the succeeding whorl. At 14 Fronjbier formation. The associated species include millimeters diameter umbilical, median-lateral, mar Scaphites ventricosus Meek and Hayden, Scaphites sp. ginal, and median-ventral nodes are present, numbering undescribed, Inoceramus aff. I.fragUis Hall and Meek, on the succeeding whorl (to 39 millimeters diameter) /. stantoni Sokolow, and other pelecypois and gas 11 umbilical, 12 median-lateral, 19 marginal and me tropods. A sandstone 200 feet higher contains dian-ventral; the umbilical and median-lateral nodes are Scaphites ventricosus, Scaphites sp. undescribed (same conical, the marginal and median-ventral elongated; as above), Placenticeras pseudoplacenta Hyatt, Ino 5 of the primary ribs fork at.the median-lateral line ceramus stantoni, I. aff. /. ereeius Meek, and other of nodes (outside the mid line of the flank), and there mollusks. A third sandstone, apparently 300 feet are two intercalated secondary ribs; ribs of even height higher still but possibly a duplication of the last, throughout. At a diameter of 50 millimeters the constituting the highest member of tl 3 Frontier, umbilical and median-lateral nodes, both blunt conical, contains Scaphites ventricosus, Mortoniceras shoshonense and the connecting ribs begin to increase in relative Meek, Baculites codyensis Reeside, Inoceramus stantoni, prominence and the median row shifts toward the I. umbonatus Meek and Hayden, and oth^r mollusks. umbilicus; on the other hand the secondary ribs on the A sandstone 150 feet below that containing B. stantoni outer part of the flank decrease much in prominence, contains Inoceramus sp. and fossil plants ** and is the though the marginal tubercles remain high; the base of the Frontier formation. median-ventral nodes decrease somewhat in height. Barroisiceras (Forresteria) hobsoni Reesid^ n. sp. The last half whorl of the type, from 80 millimeters to Plate 9, Figures 2-4; Plate 10, Figures 1-2 130 millimeters diameter, is much corroded, but ap parently the median-ventral nodes are distinct to the A single entirely septate internal mold with a end of the shell, the umbilical and median-lateral maximum diameter of 170 millimeters is the basis of nodes and the primary ribs fuse into a lateral rib, and this species. the marginal nodes become more prominent. Shell a stout disk, large for the genus, fo^ a complete The suture at 25 millimeters diameter shows the shell would certainly exceed 225 millimeters in diam usual character of moderate dissection; first lateral eter. Early stages unknown. At a diameter of 75 lobe subequal to the siphonal lobe; second lateral lobe millimeters the cross section of the whorl is roughly much smaller; an ill-defined, broad third lobe; first hexagonal, but in the succeeding whorl (to 170 milli lateral saddle about twice as broad as the first lateral meters) it becomes more nearly subquadrHe. Living lobe. At 65 millimeters diameter the suture is much chamber and aperture uaknown. Umbilicus wide for the same, with all the elements rather rounded the genus, 58 millimeters at a diameter of 170 milli- terminally. ineters or oa©*tibM the diameter; umbilbal shoulder B. stantoni is characterized by its relatively wide distinct and rather sharp; umbilical w«U at right umbilicus in the later stages, its stout shell with hexag angles to the flank. onal cross section of the whorl passing into sub- / Sculpture »t earliest stage seen, the half whorl from quadrate, the prominence of the umbilical and median- 70 millimeters to 90 millimeters diameter consists of lateral nodes and the connecting primary ribs, and the 7 primary ribs passing irom a very work umbilical persistence of the marginal and median-ventral nodes. node to the middle of the flank, where e<*eb, bears a In the early stages it resembles B. sevierense somewhat low but distinct node; 4 of the primary libs fork at but is much stouter at equal diameters and has more the median-lateral node and the ribs then pass to the numerous ribs. In the later stages it is somewhat like 11 rather bagfe mwgiaal nodes; from tne<*« faint ribs B. hobsoni but differs in its broader venter, the lack ran diagonally forward to the Mgh, nraeiH elongated, of large spines, and coarser sculpture. No species mediaja-vemtwJ, nodes, wMeh form a coarsely sen-ate outside of America is very close in the later stages, keel. Oa the succeeding three-fourths of & whorl (to though B. alstadenense (Sehiilter) M resembles it in 170 millimeters diameter) the umbilical nodes and the early stages,being separable by weaker sculpture primaiy libs fade oat completely; the m^iiftn-latoral and more compressed shell. B. alstadenense Solger nodes gradually change in prominence, sx> that each (not Schliiter) 89 also is more compressed and has less third node Incomes * largo blunt spine an 4 the others conspicuous median-lateral nodes. weaken; the spines move outward, so that the last preserved is nearly flush with the ventral surface; the SB SehlGter, Clemens, op. cit., p. 151, pi. 40, figs. 13-16. Grossouvre, Albert de, op. cit., p. 51, pi. 1, fig. 4, pi. 2, fig. 4. to Berry, B. W., The flora of tfce Frontier fonBattoa: 17. 8. (ted. Survey Prof. s» Solger, Friedrich, op. cit., p. 170, pi. 5, fig. 6. Paper 158, pp. 129-136, pis. 30-21,1930, THE tJPPEB CRETACEOUS GENUS BARBOI8ICERAS marginal nodes become coarser and blunt but relatively calated. All these ribs are plainer on the es*I lower; the median-ventral nodes begin to lose their of the whorl and decrease in distinctness distinctness, at least on the internal mold, and appear later part, suggesting that still later whorls to unite in a nearly smooth low keel. smooth. The parts of the earlier whorls seen, p«ttfou- Suture not well preserved, but enough may be larly from 4 to 11 millimeters diameter, show about discerned to show a long, slender first lateral lobe; first 25 distinct ribs per whorl on tiie outer part of tlw* flank, lateral saddle nowhere clear but seems to be about though the umbilical part shows only weak, distant twice as wide as the first lateral lobe; second lateral ribs and no nodes. On the outer whorl the rather lobe small and near the umbilical shoulder. obscure ventrolateral shoulder is marked by a row of B. hobsoni is best characterized by its relatively 38 rounded nodes, from which weak ribs run PLATES 3-10 21 PLATE 3 Page 1-10. Barroisiceras (Texasia) dentatocarinatum (Roemer) Lasswitz______-______— _____ — ______—— — _— 15 1-3. Side and front view and suture of the type specimen, from the Austin chalk at the falls of the Guadalupe River, 2 miles below the bridge east of New Braunfels, Comal County, Tex. (Copied from Roeraer, Die Kreidebildungen von Texas, pi. 1, figs. 2a-c, 1852.) 4-8. Front, rear, and side views, cross section, and suture at diameter of 45 millimeters of a small, entirely septate internal mold from the type locality of the species. U. S. Nat. Mus. catalogue No. 73753. 9-10. Front view and cross section of a nearly complete internal mold from the Austin chalk on Verde Creek, 8 miles north of Hondo, Medina County, Tex. U. S. Nat. Mus. catalogue No. 73754. 22 U. S. GEOLOGICAL SURVEY PROFESSIONAL PAPEE 170 PLATE 3 SPECIES OF BARROISICERAS TJ. S. GEOLOGICAL SURVEY PEOPESSIONAL PAPER 170 PLATE 4 SPECIES OF BARROISICERAS PLATE 4 Pago 1—3. Barroisiceras (Texasia) dentatocarinatum (Roemer) Lasswitz______-______15 1-2. Peripheral and side views of a fragment from the Austin chalk on Cow Creek below Pinto Creek, about 24 miles below Del Rio, Tex. U. S. Nat. Mus. catalogue No. 73755. 3. Side view of specimen shown in Plate 3, Figures 9-10. 4-8. Barroisiceras (Alstadenites) sevierense Reeside, n. sp., side, front, and rear views, cross section, and suture at diameter of 42 millimeters of the type, an entirely septate internal mold from the Mancos shale, 200 feet above the top of the Ferron sandstone member, at a locality in Sevier County, Utah, 4 miles east of Oak Spring and 12 miles south west of Emery. U. S. Nat. Mus. catalogue No. 73756_--_-_____-___-______16 23 PLATE 5 Page 1. Barroisiceras (Texasia) dentatocarinatum (Roeiner) Lasswitz, side view of specimen shown in Plate 3, Figures 9-10, with part of outer whorl removed-______15 2-7. Barroisiceras (Forresteria) forresteri Reeside, n. sp., two side views, front and rear views, cross section, and suture at diameter of 36 millimeters of the type, an entirely septate internal mold from the Mancos shale, 200 feet above the top of the Ferron sandstone member, at a locality in Sevier County, Utah, 4 miles east of Oak Spring and 12 miles southwest of Emery. U. S. Nat. Mus. catalogue No. 73757______17 24 PROFESSIONAL PAPER 170 PLATE 5 TJ. S. GEOLOGICAL SURVEY SPECIES OF BARROISICERAS U. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 6 10 SPECIES OF BARROISICERAS PLATE 6 1-5. Barroisiceras (Harleites) castellense Reeside, n. sp., side, rear, and front views, cross section, and suture at diameter of 36 millimeters of the type, an entirely septate internal mold from the Mancos shale, 200 feet above the top of the Perron sandstone member, at a locality in Sevier County, Utah, 4 miles east of Oak Spring and 12 miles southwest of Emery. U. S. Nat. Mus. catalogue No. 73758------19 6-7. Barroisiceras sp. Side and rear views of an internal mold retaining parts of the shell from the Austin chalk on Cow Creek below Pinto Creek, about 24 miles below Del Rio, Tex. U. S. Nat. Mus. catalogue No. 73759---- 19 8-10. Barroisiceras (Texasia) dartoni Reeside, n. sp., side and front views and cross section of the type, an internal mold from the Austin chalk near the Sabinal-Utopia road, 5 miles north of Sabinal, Uvalde County, Tex. U. S. Nat. Mus. catalogue No. 73760______.______-___ 16 25 PLATE 7 Page 1-7. Barroisiceras (Forresteria) stantoni Reeside, n. sp., from the Frontier formation in T. 33, N., R. 99 W., southeast of Lander, Wyo. TJ. S. Nat. Mus. catalogue No. 73761______17 1-2. Front view and suture at diameter of 60 millimeters of the type, an internal mold showing part of the living chamber. 3-7. Side, front, and rear views, cross section, and suture at diameter of 27 millimeters of the paratype, a small internal mold retaining traces of the shell. 8-9. Barroisiceras (Texasia) dartoni Reeside, n. sp., side and rear views of the specimen shown in Plate 6, Figures 8—10___ 16 26 U. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 7 SPECIES OF BARROISICERAS IT. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 8 SPECIES OF BARROISICERAS PLATE 8 Page 1—3. Barraisiceras (Forresteria) siantoni Reeside, n. sp., side and rear views and cross section of the specimen shown in Plate 7, Figures l-2______17 27 PLATE 9 1. Barroisiceras (Forresteria) stantoni Reeside, n. sp., side view of the specimen shown in Plate 7, Figures l-2______17 2—4. Barroisiceras (Forresteria) hobsoni Reeside, n. sp., front and rear views and suture of the type, an entirely septate internal mold from the Timpas limestone, of Niobrara age, near Carlile Springs, Colo. U. S. Nat. Mus. catalogue No. 73762______18 TJ. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 9 SPECIES OF BARROISICERAS TJ. S. QEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 10 t N l\ t\ \ \ \ SPECIES OF BARROISTCERAS PLATE 10 Page 1—2. Barroisiceras (Forresteria) hobsoni Reeside, n. sp., side view and cross section of the specimen shown in Plate 9, Figures 2-4_____.______,______.______.______.. 18 29 A MIOCENE FLORA FROM GRAND COULEE, WASHINGTON By EDWARD WILBER BERRY INTRODUCTION prevailed over a very great area of country in Idaho, The fossil plants described in the present report were Washington, and Oregon during late Miocene trme. collected at the north end of Grand Coulee during the In all 55 different types of plants have been recog summer of 1927 by Messrs. T. A. Bonser, F. A. Roberts, nized in the material from Grand Coulee, or about one- and Walter Bruee, of Spokane, and F. W. McCann, third the number described from the Latah fonration. of Coulee City. The locality is in the big bend of Several of these, however, are not distinct species but the Columbia River near the northern boundary of comprise such things as maple keys, taxodiurr cone Grant County, Wash., about 85 miles west of the plant- scales and staminate catkins, oak acorns and cruules, bearing Latah sediments around Spokane. The out poplar bud scales, and a sycamore flower head, which crop in Grand Coulee is about the same distance east undoubtedly appertain to the associated botanic species of the crest of the Cascade Mountains, about 100 miles based on foliage. northeast of the plant beds at EUensburg, which are of They represent 34 genera in 25 families and 10 orders. approximately the same age, and some 200 miles west Five of the genera are gymnospermsj the remainder of beds in Idaho yielding a similar flora and assigned are angiosperms. All but one of the fyngiosperriis are to the Payette formation by Knowlton and others. dicotyledons, and all of these except the V$bvnmm The material in which the plants occur is of two not belong to the choripetalous division. The moist abun* very dissimilar sorts. One is a buff diatomaceous dant individually are the leaves of birch, dhesteut, elm, matrix which I am informed occurs as boulders in poplar, and oak. Severn different species of oakt hitve glacial till. The other is a ferruginous clay found in been named, but it should be pointed out thaf< ttoe place, which might well be a more silty phase of the has probably been an overrefinement ia species due to- diatomaceous rock. the personal equations of the different students who- The following details concerning the geography and have worked on Miocene floras, to the great variability geology of the plant-bearing deposit were furnished by of the leaves in this and other genera, such as Betula, Mr. T. A. Bonser, of the Spokane Public Museum: Ulmus, and Acer, and to the practical impossibility of drawing specific lires tiiroughout where large anounts The clay deposit in which the fossil leaves occur is at the extreme north end of the coulee, just at the top of the hill that of material are available for study. leads down to the Columbia Elver. It is on a level with the The flora thus far discovered at Grand Coulee does floor of the north end of the coulee and about 600 or 600 feet not add anything to the conclusions regawiiE^ erviron- above the river. The winding road from the floor of the coulee mental conditions, which were set forth at some length. to the river is about 2 miles long, but the actual distance from in my discussion of the Latah flora.1 Most of the> the deposit to the river is not more than half a mile. The deposit rests upon granitic rocks, just as the Latah formation genera represented no longer occur in this genwal re does in the neighborhood of Spokane. Detached clay boulders gion. Many have become entirely extinct in vestem in a glacial till about half a mile down the hill along the road North America since the Miocene epoch, and a few, also contained fossil leaves. such as Glyptostrobus and Paliurus, are confined to the: The principal exposure is about 200 yards long and 15 to 20 Old World in existing floras. feet deep at the highest point, but there is evidently a much greater depth below the level of the road. On a ranch about a Inasmuch as the flora discovered at Grand Coulee quarter of a mile northwest of the exposure and about 50 to 80 can be rather closely correlated as to age and as it ia feet higher fossil leaves were found in an excavation for a cellar. but a small part of the Miocene flora of western North To the southeast of the plant locality th4re is a basaltic rock America as a whole, an attempt to discuss the I *»ader wall standing 800 to 1,000 feet above the floor of the coulee, and questions of its antecedents, environment, extinction, several miles southwest is the locally famous Steamboat Rock, about 800 or 1,000 feet high. and bearing on the geologic history of the region does not seem worth while. This has been done to The plant material is not as abundant, as varied, or some extent in connection with the Latah flor*, and as well preserved as that of the Latah formation at permanent results can be reached only after the large Spokane, Wash., but it is of considerable interest in amount of material from tfee Pacific States wMch is that it furnishes several species that are new to the being studied by Chaney, me, and others has been flora of our western Miocene. In addition, it greatly fully worked up and published. extends the range of many of the already known species > Berry, E. W., A revision of the flora of the Latah formation: IT. 3. Oft. Survey and shows that essentially similar physical conditions Prof. Paper 154, pp. 233-234,1929. 31 32 SHOBTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 AGE OF THE GRAND COULEE PLANTS is not the place to attempt a discussion of these Idaho The Grand Coulee flora can be correlated with great floras beyond making clear the qualification required precision. Of the 55 objects enumerated in the accom by the present state of our knowledge in comparing the panying table of distribution 48 occur in the Latah Grand Coulee plants with those identified or reported flora around Spokane, those that have not as yet been from Idaho localities. recorded from the Latah being Glyptostrobus europaeus, Twelve of the Grand Coulee plants are recorded Hicoria washingtoniana, Juglans egregia, Lysichiton from the Mascall formation of Oregon, and it seems washingtonense, Platanus flower head, Ptelea miocenica, probable that this number will be increased when Quercus mccanni, and Vitis bonseri. Of these the Chaney completes his revision of this standard flora Hicoria, Lysichiton, Ptelea,, Qwrcus, and Vitis are new and especially when the personal equation^ of various and are likely to turn up at any moment in the Spo- students in connection with such genera as Acer, iane area. Moreover, the Platanus flower head, the Liguidambar, Betula, and Ulmus are taken into account. fragment of a Lysichiton spadix, and the Vitis seed may Seven of the Grand Coulee plants are recorded from be classed as more or less exceptional and accidental^ the Eagle Creek formation, and these seeti to me to both as to original preservation and as to subsequent indicate that the Eagle Creek is somewi H younger -discovery. Juglans egregia is a species of the, Cali than it is generally held to be. fornia Miocene, and I have seen it in collections from Only four of the Grand Coulee plant® s re recorded Idaho. The Glyptostrobus has thus far unaccountably from Morissant, Colo., but of these the Popu&us and not been found in the Spokane region, but it will Liguiclambar are significant. As the Gr^nd Coulee probably turn up there eventually, for it is not uncom flora is practically identical with that frcm Spokane mon in the western Miocene and is present in the its real similarity to the Florissant flora muft be greater Payette formation of Idaho. Consequently there than it seems, for the Spokane flora has a great many -can be no doubt that the Grand Coulee flora is of the elements in common with that at Morissr.nt and the same age as the Latah flora of eastern Washington. later and unpublished collections from Spokane indi Next to the practical identity of the Grand Coulee cate that this resemblance is still stronger. flora with that of the Latah the greatest resemblance I consider that five of the Grand Coulee plants are is shown to floras recently collected by Kirkham in represented in the flora from the St. Eufjene silt of west-central Idaho and submitted to me for identifica the Kootenay Valley, in British Columbir, described tion. The localities with lists of species have been by Hollick.3 I have already commented briefly on described in a recent paper by Eorkham and Johnson.2 this,4 and a more complete discussion is not called for These authors consider the Latah a series rather than a in the present connection, but the great aHmdanee of formation and extend the name to include not only Cebatha heteromorpha in both floras seem'* to la® to their Idaho localities but the Grand Coulee locality, settle beyond dispute the age of th« Canad'ftn deposit. which they had heard of through Mr. McCann, of The position to be assigned to the Gr^wd Coulee Coulee City. In the accompanying table of distribu flora in the world section of the Tertiary is tied up with tion I have listed the Idaho occurrences as from the the results of the study of the other scatter^ Miocene Payette formation, though I believe the plant-bearing floras of the westeiii TJioltecl States. In my published Tseds in Idaho represent several horizons, and. I account of the Ijatfth; flora I stated my belief that question the propriety of using the name Latah there. although the LaAaa Jaifght'be as old as imdcUe Miocene If all the disconnected basins of sedimentation associated it was jeaore-ppol^iWy Tipper Miocene, In the several with the Columbia River lava are to be called by a years that have elapsed since the manuscrSt for that single name, which I do not believe is the proper pro account was prepared I have studied numerous addi cedure, there are other and earlier names than Latah— tional collections from tib® Spokane, area, and nothing for example, Payette (1898), Ellensburg (1900), and I have seen in these later, collections har served to Mascall (1901). But it is not clear that the Payette modify this statement. On the other hard, the evi beds are more than partly equivalent to the Latah. dence for an a^per Mioeifie age h constantly becomiag Certain plants from the Idaho section suggest a Plio more eomviadWg. ,$£&1bei&g tne ease for t\e Spokane cene age, and there are some elements identical with flora, so mudfe more extensive and better the Bridge Creek flora which do not occur in the than the Grand Coulee flora, the same ccmcl Spokane area and which suggest that a part of the equally for the Grand Cowlee. Idaho section is older than the typical Latah. This * HoUiek, Arthur* Tbe flora of the St. Eugene silts, Kootenaj- Valley, British Columbia: New York Bet. Qard^aiettt,, vol. 7, pp. S8BHW4, pto, 2SM7,1SS7. 2 Kirkham, V. R. D., and Johnson, M. M., The Latah formation in Idaho: Jour. * Berry, 1. W., The age ot&M.8t, Bngene silt te.th* KoBtense* Valtey, British -Geology, voL 37, pp. 483-504,1929. Columbia: Boy. Soc. Canada, see. 4, Trans., M atr.,' vel. 23, pp. 47-48,1829. A MIOCENE FLOEA FROM GRAND COULEE, m Flora from Grand Coulee, Wash., compared with Miocene floras from other Idealities Latah for Payette for Eagle Miocene of St. Eugene mation, Mascall Ellensburg Bridge YeBow- Florissant, Spokane formation formation mation of Creek flora Creek for Colo. California silt. Brftfeft and vicinity Idaho mation stonePark Oa.nabia Acer merriami ______V v v Acer, fruit ______v Betula heteromorpha- _ CD Betula large! ______Carpites boraginoides ______V Carpites ginkgoides _____ Cassia spokanensis ______X Castanea castaneaefolia___ _ v X Cebatha heteromorpha ______X X X v v Ficus interglacialis______v X Hicoria washingtoniana. .. ___ Juglans egregia______v Libocedrus praedecurrens______X (?) v Liquidambar, fruits ______v Menispermites latahensis ______X Nyssa hesperia ______v Nyssa magnifica. ______Paliurus hesperius ______X v Platanus aspera ______v Platanus dissecta ______V v X (?) v v V v v Populus, bud scales______X X Prunus rusti_____-_--______v v . v v v -^ (?) v V Quercus simulata ______v v v v v v X v v v v v V v v v X * v Viburnum f ernquisti. ______— _ _ _ v 34 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 A systematic list of the species identified in the Spermatophyta—Continued. Grand Coulee flora is given below, as it has not seemed Angiospermae—Continued. Dicotyledonae—Continued. necessary to describe any except those that are new or Choripetalae—Continued. afford some addition to our knowledge. Rosales—Continued. Coniferophyta: Drupaceae: Finales: Prunus rusti Knowfton. Cupressinaceae: Caesalpiniaceae: Sequoia langsdorfii (Brongniart) Heer. Cassia spokanensis B^rry. Taxodium dubium (Sternberg) Heer. Papilionaeeae: Taxodium, cone scales. Sophora alexanderi Knowltofl. Taxodium, staminate aments. Sophora spokanensis Knowlton. • Libocedrus praedecurrens Knowlton. Geraniales: Glyptostrobus europaeus (Brongniart) Heer. Rutaceae: Pinaceae: Ptelea miocenica Bery. Tsuga latahensis Berry. Sapindales: Spermatophy ta: Celastraceae: Angiospermae: Euonymus knowltoni Berry. Monocotyledonae: Aceraceae: Arales: Acer merriami Know?ton. Araceae: Acer, fruit. Lysichiton washingtonense Berry. Rhamnales: Dicotyledonae: Rhamnaceae: Choripetalae: Paliuras hesperius Bony. Juglandales: Vitaceae: Juglandaceae: Vitis bonseri Berry. Juglans egregia Lesquereux. Parietales: Hicoria washingtoniana Berry. Ternstroemiaceae: Salicsles: Gordonia hesperfa BrTy. Salicaceae: Laurales: Populus lesquereuxi Cockerell. Lauraceae: Populus washingtonensis Knowlton. Laurus similis KnowJton. Populus lindgreni Knowlton. Umbellularia lanoeolata Beery. Populus, bud scales. Umbellales: Betulaceae: Cornaceae: Betula heteromorpha Knowlton. Nyssa magnifica Knowlton. Betula large! Knowlton. Nyssa hesperia Berry. Gamopetalae: Castanea castaneaefolia (Unger) Rubiales: Knowlton. Caprifoliaceae: Quercus payettensis Knowlton? Viburnum feraquisti Berry. Quercus pseudolyrata Lesquereux. Position uncertain: Quercus merriami Knowlton. Carpites ginkg0M*s Knowlton. Quercus cognata Knowlton. Carpltes boraglooides Knowlton. Quercus mceanni Berry. PhylUtes amplexieaulis Knowlton. Quercus, acorns and cupules. Phyffites couleeanus Berry. Quercus treleasi Berry. Quercus simulata Knowlton. SYSTEMATIC DESCBIFnONf Urticales: Phylum CON1PEEOPHYTA Ulmaceae: Ulmus speciosa Newberry. Order FINALES Moraceae: Family CUPRESSINACEAE Ficus washingtonensis Knowlton. Ficus interglacialis Hollick. Genus TAXODIUM I. C. Eichard Platanales: Taxodlttm dttblum (Sternberg) He«r Platanaceae: Platanus dissecta Lesquereux. Plate 11, Figure 1 Platanus aspera Newberry. Platanus, flower head. The more or less complete synonymy cf this ubiqui Ranales: tous species has been repeatedly publisl^ in recent Menispermaceae: years and need not be repeated in the present con Menispermites latahensis Berry. nection. Cebatha heteromorpha (Knowlton) This species was discussed and a number of illus Berry. Resales: trations were given in Knowlton's account of the Grossulariaceae: Latah flora.6 Ribes fernquisti Berry. i Knowlton, F. H., Flora «t the Latah formation of Spofeano, Wasb., sad Coeor Hamamelidaceae: d'Ateae, Idaho: U, S. Geol. 8arv«r Prof. Paper 140, p. 27, pi. 9, flgs. 2, 7~8j pi. 01, Liquidambar, fruits. fig. 2, im. A MIOCENE FLOBA PBOM GRAND COOTEE, WASHBf«1?0N The leafy twigs are sparingly represented at Grand single botanic species as illustrated among exiting Ooulee. Associated with these are excellently pre forms. served cone scales, which do not differ appreciably from those of the recent species of southeastern North Amer Genus HICOBIA Bafineaque ica. One of these from Grand Coulee is figured on the Hicoria washlngtoniana Berry, n. sp. accompanying plate. Plate 11, Figure 4 There also occur in the Grand Coulee deposits stami- nate aments of Taxodium exactly like those that have This species is based upon the single incoir'^lete proved to be so common in the Spokane region. specimen figured. The material scarcely warrant an attempt at a diagnosis, but as it differs from tite large Phylum SPEBMATOPHYTA amount of material of this age from Washington and Class AKGIOSPERMAE Idaho which I have studied it seems worthy of record, Subclass MOKOCOTYLEDOKAE The specimen is interpreted as a terminal leaflet of a Order AEAIES large-leaved species of hickory, although it is not pos sible to be sure that Hicoria and Juglans have not been Family ABACEAE confused in this case as they have been in the ps«t by Genus LYSICHITOK Schott other authors. The specimen indicates an ovat^ leaf Lysichiton washingtonense Berry, n. sp. about 16 centimeters in length and 6 centimeters in Plate 11, Figure 2 maximum width. The midveia is stout and promi This species is based upon the impression of a tiny nent. The secondaries are relatively widely sj i,ced, specimen which appears to represent parts of a crushed stout, diverging at angles of 45° or slightly more, regu spadix of some aroid similar to or identical with larly ascending, and camptodrome. The tertiari.es are Lysichiton. It shows the impression of the surface, indistinct but form an open areolation. The margins which is seen to consist of small individuals (carpels?) are beset with fairly large, uniform, closely spaced closely packed and polygonal in outline, about 1 milli crenate teeth. The texture is fairly coriaceous. meter in diameter, highly convex distad, with a pro Comparison of such incomplete material with either nounced central umbilicus. The type and only speci living or fossil species is worth little. In some reflects men is shown enlarged in the accompanying illustra it suggests the leaves of the Ternstroemiaceae, Ixut it tion. is larger and relatively wider than the members c f this The genus Lysichiton, the sole survivor of the Araceae family in the western Miocene which I have referred in western North America, has but one or two exist to the genus Qordonia. ing herbaceous species, ranging from eastern Siberia The genus Hieona has been recorded in the F^ific through Alaska and western Canada to California and region from the Miocene of Colorado, California, Spo Idaho. It is unfortunate that more complete material kane, Wash., British Columbia, and Oregon. It is, of of the fossil form is not available, but it must be con course, present also in beds representing earlier hori sidered to be a matter of extreme luck that even a frag zons in this general region. ment was preserved and discovered. Order SALICALES Subclass DICOTYLEDOKAE Genoa POPTOUS Series CHOBIPETALAE Populus lesquereuxi CockereU Order JUGIAKDALES Populus heeri Lesquereux, The Cretaceous and Tertiary floras, Family JUGLAHDACEAE p. 161, pi. 30, figs. 1-8; pi. 81, fig. 1 1, 1883. [Not Sa->orta.] Poptdus lesquereiai Cockerell, Torrey Bot. Club Bull., vol. 33, Genus JtTGIANS Linn§ p. 307, 1906; Colorado Univ. Studies, vol. 3, p. 172. 1906; Juglans egregia Lesquereux Am. Naturalist, vol. 44, p. 44, fig. 8, 1910. Knowlton, U. S. Nat. Mus. Proc., vol. 61, p. 261, 1916. Plate 11, Figure 3 Salix inquirenda Knowltoh, U. S. Geol. Survey Prof. Pap^r 140, Juglans egregia Lesquereux, Harvard Coll. Mus. Comp. Zoology p. 32, pi. 11, figs. 1, 2, 1926. Mem., vol. 6, p. 36, pi. 9, fig. 12; pi. 10, fig. 1, 1878. Berry, U. S. Geol. Survey Prof. Paper 154, p. 242, 1929. Knowlton, in Lindgren, Jour. Geology, vol. 4, p. 889, 1896. The Latah species named Salix inquirenda, by Knowl This species was described by Lesquereux from the ton is represented by very large leaves at Grand Coulee auriferous gravel of California and was based upon a and appears to me to be identical with the common considerable amount of fairly complete material show Jlorissaiit form which. Lesqmerewx determined as Popu ing much variation in size and some variation in form, lus heeri Saporta but%Heh Coekerell has shown to be particularly respecting the obtuseness or pointedness different from that European species. The extremely of the base. As might be expected, the broader leaves long and stout petiole, which is preserved, in mT*eh of are obtuse and the narrower acute, but such variations my material, is also eonfirmatory of the refererne to as have been observed are well within the limits of a Populus instead «f to Soliz. 36 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 Order FAGALES America, and this agreement is so close tl ^t it would Family FAGACEA1 seem to indicate a close relationship and tlje former presence in the late Miocene of the West of a type of Genus QUERCUS Linne oak which subsequently became restricted to the, East. Quercus mccanni Berry, n. sp. A second alternative m indicated by the resemblance Plate 11, Figures 5-7 of these leaves to those of the existing £ wrem mar- tensiana Trelease, of the eastern Sierra Ma*ire, Qwr&us Leaves lanceolate to obovate, with an abruptly prinopsis Trelease, of the Mexican tableland, and pointed apex and a base that varies from cuneate to Quercus chartacea Trelease, of the CordiTwan region truncately rounded and in many specimens is inequi of Mexico. • lateral. Most of the specimens are preserved as Quercus simnlata Kuowlton impressions, but in the two or three that show some Quercus simulata Knowlton, U. S. Geol. Survey Eighteenth thing of the leaf substance the texture appears to Ann. Kept., pt. 3, p. 728, pi. 101, figs. 3, 4-; pi. 102, figs. have been subcoriaceous, though less so than in the 1, 2, 1898; U. S. Geol. Survey Prof. Pap^r 140, p. 38, associated species of oaks. Margin entire for a very pi. 22, figs. 3, 4, 1926. ] Chaney, Walker Mus. Contr., vol. 2, No. 5, p. 168, pi. 12, short distance above the base; elsewhere with regular fig. i, 1920. spaced and sized teeth. These increase regularly in Berry, U. S. Geol. Survey Prof. Paper 154, p. 24§, pi. SI, size upward to the widest part of the leaf and then figs. 6, 7, 9-11, 1929. decrease toward the apex. They are usually oblique Scdix elongata Knowlton [not O. Weber], U. S. Geol. Survey and rounded and are separated by rounded sinuses, Prof. Paper 140, p. 32, pi. 12, fig. 4, 1926. Quercus chaneyi Knowlton, idem, p. 38, pi. 22, fig. 1, 1926. the counterpart of the teeth in form. In one or two Quercus praenigra Knowlton, idem, p. 37, pi. 19, fig. 6, 1926. of the more elongated and narrower leaves the teeth This species was described by Knowlton from the are more ascending and pointed, and these leaves are Payette formation of Idaho and was identified by the very similar to those of Quercus horniana Lesquereux, same author from the Latah formation and by Chaney of the Mascall formation of Oregon, but the Grand from the Eagle Creek formation. I hr.ve recently Coulee leaves are connected by insensible gradations detected it in the Esmeralda formation of Nevada. with the round-toothed forms with which they are It is exceedingly common and variable in both the associated and undoubtedly represent a single botanic Payette and Latah formations. At Granc? Coulee it is species. Petiole stout, expanding proximad, 1.2 to 2 probably the most abundant species, and here again centimeters in length. Midvein stout, prominent it shows its characteristic great variability both in on the underside of the leaf, becoming thin distad. form and in size. It ranges from narrowly to broadly Secondaries medium stout, regularly spaced, and sub- lanceolate, with entire or sparingly toothed margins, parallel; their angle of divergence from the midvein either acuminate or bluntly tipped and with the base depends on the width of the leaf, varying from 40° to ranging from rounded to narrowly cuneate. Formerly 60°; they are prevailingly straight, curving slightly I suggested comparisons with the existing ($wrem distad and ending craspedodromely in the tips of the hypoleuea EngebaaBJt 13! the West or Qmrms pheUos marginal teeth. The tertiary venation is quercoid, Linne ot the East. not prominent and seen with difficulty. Length 6.5 to I have subsequently had occasion to compare this 10 centimeters; maximum width, above the middle, and oar otiaejr western Miocene oafes with the existing 2.75 to 5 centimeters. species df Meaaeo au.4 Central America, witfo t3to result This characteristic species, which is named for JP.W. titiftt I find a great siiiHlarity between Qmr&m simulata McCann, president of the Coulee City Commercial and & gfwift 0f M««ki«fr^^®cies, mut&j of them shrubs Club, is obviously distinct from previously described or small trees, largely described in recent years by forms, although it exhibits a certain resemblance to Trelease. These &re Qj&eFcm v&apulcengw Trelease, Quercus horniana, Lesquereux,6 of the Mascall forma Quercus <$§eww Trelease, $mrm$ transm&ntana Tre tion, Quercus spokanensis Knowlton,7 of the Latah lease, (^mrm» mmi/Am Release, and Qmm$ hypoleuea, formation, and Quercus clarnensis Trelease,8 of the Engelmanii, the last akeady mentioned in the preced Clarno formation. This resemblance is greatest be ing paragraph. All of these are forms of the western tween these species, which are narrower forms with more Sierra Miulre. la addition tymrcm m&e^&n® Hum- pointed and more ascending teeth, and the more elon boldt and Bonplaiid is also similar to the fossil form. gate and narrow specimens of Quercus mccanni. This is ft sjjcutesiqf;^fcp'-Mi«ieaa:i table4aiid and adja In all its features Quercus mccanni is exceedingly like cent Cordillera. This Te&emblance between several of the leaves of the chestnut oaks of southeastern North the oaks of the western Miocene and existing species « Lesquereux, Leo, U. S. Nat. Mus. Proc., vol. 11, p. 17, pi. 6, flg. 6, 1888. of Mexico seems M to 1 wore tibtan fortuitous, and I i Knowlton, F. H., U. S. Geol. Survey Prof. Paper 140, p. 37, pi. 19, flg. 3,1926. " Trelease, William, Brooklyn Bot. Garden Mem., vol. 1, p. 499,1918. believe that it is of real significance. A MIOCENE FLOBA PBOM GRAND COULEE, Quercus treleasii Berry Order FLATANALES Qwercus trdeasii Berry, U. S. Geol. Survey Prof. Paper 154, Family PLATANACEAE p. 247, pi. 52, figs. 1-3, 1929. PLATANUS Linne" This species is abundant in the Latah formation and also in the recent collections from, beds assigned to the Plateaus, flower Payette formation of Idaho. It is represented at Plate 12, figure 1 Grand Coulee by a single specimen. Like some of Little that is definite can be said of this the associated oaks, Quercus treleasii shows similarities which appears to represent a flower of Plat The older paleobotanists referred to Populus a great Order EOS ALES many fossil leaves which show no relationship to that Family GROSSULAKIACEAE genus. Knowlton in his account of Populus hetero- morpha recognized that it was unlike any existing Genus RISES Iinn6 Populus but convinced himself that it was a Populus Ribes fernqaisti Berry because it resembled Populus ardica Heer of the early Plate 12, Figure 2 Tertiary, a species which I have shown is also not a Ribes femquisti Berry, U. S. Geol. Survey Prof. Paper 154, p. Populus. 251, pi. 63, fig. 21, 1929. Genus MENISPEBMITES Lesquereux This species was described as follows: Menispermites latahensis Berry Leaves relatively small, trilobate. Margin, except at base Rate 12, Figures 4-6 and in the sinuses, with c'oarse den ;ate teeth. Texture sub- coriaceous. Length about 5 centimeters, as is also the maxi Menispermites latahensis Berry, U. S. Geol. Survey Prof. Paper mum width. Apical lobe about as broad as it is long, bluntly 154, p. 249, pi. 52, fig. 4, 1929. pointed at apex. Base of the leaf truncate. Sinuses narrow Leaves relatively small, about as long as their maxi and not deep. Primaries, three from the top o* the petiole, mum width, trilobate, with a wide central lobe and a stout and prominent. Secondaries si out, prominent, diverging from the primaries at acute angles. There are three or four" pair of basal lateral lobes. Sinuses rounded, extending subopposite to alternate secondaries i Q the central lobe, curved inward about halfway to the midvein. Margin with proximad and more straight distad, and craspedodrome. In shallow, irregularly spaced dentate teeth, most promi the lateral lobes the basal secondary on the outside diverges nent toward tip of central lobe and on the proximal close to the base and is relatively strai ghter and more prominent side of the lateral lobes. Apex rounded. Tips of than its fellows and might be termed i subpranary. There is a second secondary on the outside belcw the basal secondary oa lateral lobes rounded, asymmetric. Base perfoliate. the inside, and the latter is much cu -ved, ascend'ng inside the Texture thin. Length about 4.8 to 6 centimeters; sinus margin and ending camptodrort ely if the margin is entire maximum width, across lateral lobes, 5.25 to 8 centi and craspedodromely if it has aseende i to a point where there ia meters. Petiole stout, presumably long, though pre a tooth on the margin. The primaries, partieuarly the lateral served for only 1.25 centimeters. Primaries stout, ones, are slightly flexuous with resp« ct to the alternate diver gence of the secondaries. The tertiary branches from the diverging from the base at angles of about 45° to 50°, distal parts of the secondaries are wel] marked, and the ultimate the laterals curving outward to the tips of the lateral ones are usually craspedodrome. Inlernal tertiaries are trans lobes. Secondaries numerous, ascending, indifferently verse and percurrent or inosculating ii i the middle region. The camptodrome or craspedodrome according as the areolation is an open mesh that agnes precisely with that ia margin at their extremities is entire or toothed. leaves of existing members of the gem is. Areolation large, polygonal. The single specimen detected in the collections from This species was apparently not uncommon at Grand Coulee is still samaller thato the type material, Grand Coulee in late Miocene time, and the three measuring 2.5 centimeters in length and 2.6 centi specimens collected are about 50 per cent larger than meters in maximum width.. Otherwise it is identical the type material from Spokane, with which they agree with the material from Spokane. perfectly in form and venation. They are not unlike Ribes has not oftett been recognized in the fossil state. some of the modern forms that American botanists Two species have, however, been recorded from Mor- refer to the genus Cebatha Forskal, which the Euro issant, C»I&., but both oi these are unlike the Latah peans generally include in the large genus Coeculus form. There are over 60 existing species of Ribes, all De Candolle. They are also similar to some of the shrubby and widely distributed in the Forth Tem forms referred to Menispermum Linn&, which, as now perate Zone and in the Andes of South America. restricted, includes an existing species in eastern Fully 50 species are knowa from North America, North America and another in eastern Asia. In view of the uncertainty of the generic affinity I prefer to Family EAHAMELtDACEAE refer the fossil to the form genus Menispermites, pro Gemus IIQTJIBAMBAR posed by Lesquereux to fit just such cases. Liquldambar, fruit Leaves of this family are common in the Upper Cretaceous of western North America but are ex Liquidambar, firttft, Kwwrite, W.-S. Ck»L Sourer Prof, Paper tremely rare in the Tertiary of that region. The 140, p. 4% pL 40, fig. Ift ISm. present species is not only a link with the past but also Knowlton described <*•& igured a rather well pre a link between eastern Asia and eastern North Amer served fruit from the IA*I& formation at S lokane and ica, where its descendants still survive. suggested its prob«W« ;pdatiQnsMp to the associated A MIOCENE FLORA FBOM GRAND COULEE, leaves, which he identified as Llguidambar pocky- Order SAPINDALES phyUum Knowlton but which I regard as simply a Family ACERACEAE variant of the common Miocene Liquidambar cali* fornicum Lesquereux. Subsequently additional fruits Genus ACM Linne have been collected from the Latah formation. I Acer merriaim Knowlton have no doubt that these fruits belong to this species. The material from Grand Coulee is especially in Plate 13, Figure 13 teresting, as there are no traces of leaves in the col Acer m&rriami Knowltoa, U. S, Geol. Survey Bull. 204, p. 74, lection and over a dozen of the fruits. In several pi. 14, fig. 7, 1902; U. S. Geol. Survey Prof. Patter 140, specimens more or less of the peduncle is preserved. p. 45, pi. 28, fig. 1, 1926. This is unusually stout, and in one small specimen The maples from the western Miocene are ia _'a in which it appears to be complete it is only 4 centi state of confusion, too many species have meters in length. The presence of fruits and no scribed, and specific names have also usually i leaves may be explained as due to water transporta given to the detached fruits. The present tion of the material, for the fruits are dry when shed are referred to Acer merriami because they; are De and readily float, and the leaves decay in water more cidedly 3-lobed and have but three primaries, al 4Hough rapidly than leaves of most other genera. I do not regard either of these features as good spe cific characters. The specimen figured di$fer" from Order GERANIALES the type in the narrower lateral lobes, in conscnuenc© Family EUTACEAE of which the base is cuneate instead of cordate, a very simple variation and of no specific value. In this Genus PTEIEA linne last feature it resembles the leaf from the Lftt«h for Ptelea miocenica Berry, n. sp. mation which Knowlton referred to this specie, Plate 12, Figure 7 Of tor EHAMU ALES Samara broadly winged, subcircular in outline, emarginate at both the apex and base. Peduncle Family RHAMNACEAE slender, incomplete, preserved for a length of about Genus PAIIURTJS Jussieu 6 millimeters. Seed cavity fusiform, widest above the middle and more tapering proximad than distad. , PaMurus hesperius Berry It has the appearance of being 2-celled. Length Plate 13, Figures 1-5 about 1 centimeter; maximum width about 6 milli Paliurus feespemts Berry, Am. Jour. Set, 5th serv vtf, 16, p. meters. The whole, including wing, about 1.75 40, figs. 1-3, 1928; TJ. S. Geol. Survey Prof- Paner 154, centimeters long and 2.4 centimeters in maximum p. 257, pi. 57, fig. 1, I92». width. The wing is thin but of firm consistency and It was my original intention, to describe tttfe leaves is faintly radiately reticulate veined. and fruits of this Palinrus as separate species. The This characteristic fruit is very close to that of the fruits were discovered and described in 1928, after* the existing Ptelea trifoliata Linne" and is the first repre manuscript for my revision of the Latah flor,^ (Pro sentative of this genus found fossil on the Pacific fessional Paper 154-H) had been prepared, aac1. in the slope. The genus makes its appearance in the lower proof of that paper (published in 1929) the aam^ given Eocene of the Mississippi embayment and is sparingly to the fruit was used for the leaves without any de- represented in the geologic record. A Miocene scription of the fraite, a citation to the earner de species based upon the trifoliate leaves has been scription being inserted. As leaves and fruits are recorded from Morissant, Colo.,9 and it is quite possible associated at Spokane and at Grand Coulee, nearly that the present fruit represents the same botanic 100 miles west of Spokaae, it is a reasonab1** con species as the leaves found at Florissant. The genus clusion that both belong to the same botanic species. is not uncommon in the Miocene of Europe. Under the circumstances the collective species should Ptelea has four or five existing species of shrubs or be redescribed. small trees confined to the United States and Mexico, Leaves of medium size, broadly qvate, wides* below ranging northward to southern Ontario and westward the middle; the apex pointed but not extended; bade to Colorado and New Mexico. broadly rounded or slightly cordate. Textoe »Coekerell, T. D. A., Am. Mus. Nat. Hist. Boll., vol. 24, p. 98,1908. " .coriaceous. Margins with closely spaced, 62508°—32——3 40 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 small, crenate teeth. Length about 7 centimeters; ure 3. Figure 1 on Plate 13 shows the fruit viewed maximum width about 4.5 centimeters. Petiole not from below pressed down over the pedur°le, which i& preserved. Midvein stout, prominent. Lateral pri seen projecting below the wing margin. In the center maries diverge from the base at acute angles; these are is the cast of the rounded apex, with a prominent con as stout as the midvein and curve upward and barely ical tip from which impressions of the veins radiate. escape being aerodrome by uniting with short second The impression is darkened around the rnargin of the aries from the distal part of the midvein. The lateral umbo, where the substance is preserved at the inner primaries give off on the outside several camptodrome margin of the wing. secondaries. The areolation is a fine mesh indistinctly The counterpart is similar except in the center, preserved. where the deep cast of the conical part of the fruit These leaves are not uncommon in the Latah forma below the wing, somewhat offset, is preserved. This tion at Spokane; they occur sparingly at Grand Coulee shows clearly the collar around the upper expanded and also in the Payette formation of Nez Perce County, end of the peduncle and the scar where its distal end Idaho, about 85 miles east of south of Spokane. was attached to the base of the fruit. The material The fruits are discoidal, peltate, pedunculate; the is almost as good as a recent Paliurus fruit and is much essential part depressed turbinate, the margin ex better for having the resistant substance of the fruit tended horizontally as a broad scarious, veined wing. proper gone, because both surfaces can be studied, one of which would have inevitably been concealed had it not dropped out when the clay was split. The fore going description is based upon the tyT>e specimen. Subsequently several somewhat smaller sp^imens have been collected from the same locality as well as from the Latah formation in the brickyard exposure at Spokane. A restoration of the species is attempted in the accompanying text figure. The fossil agrees with the fruits of the recent species of Paliurus in every feature except that it is slightly smaller, in this respect being closest to the extising Paliurus aculeatus Lamarck, although the existing forms show considerable variation in the size of their fruits, and I have not enough material to be sure of the limits of variation in either the existing or the fossil forms. The fruits of P®Mimt$ mvtmtus which I have seen are more robust, with a larger ersential part, which is much more massive proximad be1 w the wing, thicker wings, less visible venation, and shorter peduncle. The fossil is ffl«>re lake the fruits of Paliurus orientals Franca©* $*afc I nave seen, in relative pro portions, in the thinner wing with greate^ visibility of the veins, and in the relative length of the peduncle. FIGURE 3.—Restoration of Paliurus ktsperius No leaves are associated with, the fossil, but at approxi mately the same horijsem both at Grand Coulee and in The wing margin is irregularly sinuate. The veins are the Latah formation at Spokane there are leaves of a radial in direction, are slightly undulate, and may be PaKw*m whist; we meaf©r to PaMurm orwntaM® than simple or once or twice forked. they are to tibe casting species. It is very prob As preserved the whole fruit departs slightly from able that leaves »pd fraifc represent the s^me Miocene circular in outline, being about 1.2 by 1.6 centimeters species, but this ©an a&t yet be demonstrated. in diameter. The type comprises two specimens that The genus Paliurus of Jussieu contains two or three are counterparts, split in the plane of the wing, which existing species of shrubs or small trees with cordate is well preserved. The fruit substance is gone in the or ovate, palmately 3-v^ined, usually small leaves central part of both specimens and was probably lost with stipular thorns, *Ebe fruits are coriaceous, pel when the specimen was split open, as one counterpart tate, umbonate, witti a horizontal marginal radiately shows the cast of the apical umbo above the wing and veined wing. In exbtinf floras they are restricted to the other shows a cast of the proximal part below the dry-soil habitats from Spwn on,the west to Japan on. wing. These are slightly deformed by pressure during the east. Paliurus a&t^eQfm Lamarck extends from fossilization but preserve the details in a remarkable Spain through southern Europe, Asia Minor, Crimea, way and have served for the reconstructed median the Caucasus, md Peaaa to China (Szeehwan). longitudinal section shown in the accompanying Fig Paliurus mmmimmw Poiret extends frcm about 27°" A MIOCEtfE FLOBA FROM GBAND COULEE, north latitude in Kiangsi to Japan, and Paliurus sists of a typical fruit from central France (Cantal),, orientals Franchet, sometimes united with the pre which is also indistaBguiskable from the existing; ceding, reaches the stature of a thin tree sometimes 50 Paliurus aculeatus™ feet tall in eastern Szechwan and Shensi, China. In vfiew of what we know of the plant histor^ of the Whatever the taxonomic distinction of the three, the Tertiary it is surely of interest that the Miocene ranges overlap, and the geologic record is sufficiently species from Washington should be most simitar to the complete to show that their present range is a re restricted species of south-central China (P. 0r?**mteli&), stricted one and that they represent relict species. as are also the leaves associated with the friit, and Turning now to the geologic record, we may note that there should be earlier (late Eocene) species in that a considerable number of fossil species have been the intervening region in Alaska and Siberia. described, based for the most part on leaves and there fore subject to the uncertainties attending the identi Family VITACEAE fication of remains of this class. The oldest records Genus VITIS LinnS embrace 13 species, so called, of leaves from the Upper Vitis bonseri Berry, n. sp. . Cretaceous. These include four from the Dakota sandstone of Kansas, one from the Patoot beds of Plate 13, Figure 6 Greenland, two from the Mill Creek beds of western A very characteristic seed. Somewhat compressed, Canada, one from Vancouver Island, one from the broadly obovate in profile, stoutly obtusely pointed at Eutaw formation of Georgia, three from the Magothy the base, broadly rounded above. Hilum large and formation of New Jersey and contemporaneous beds circular! midway between the apex and tt*3 base; on Staten and Long Islands, and one from the so-called raphe narrow. Testa thin. Length 4.25 millimeters; "Laramie" of Yellowstone Park. Many of these are maximum width 3.5 millimeters. The single speci very similar to the leaves of the existing species but men is split medially, and the type consistr of the lack the corrobo ration of associated fruits or structural original and counterpart, which show the opposite remains. sides of the seed viewed from within. The Eocene has furnished at least 10 nominal species, In size and form the fossil is indistinguishable from including occurrences in western Greenland, Svalbard the seeds of a number of existing species of Vitis, so (Spitzbergen), Siberia, and Alaska on the north and that comparisons are without significance. in British Columbia, Montana, Colorado, and Wyo The occurrence of these characteristic seeds is of ming in the western part of North America. I have considerable interest because no leaves of this genus described three species from the Wilcox group (lower are associated with them; in fact, except for very Eocene) of the Mississippi embayment, and one of doubtful leaf material from the Latah formation at these is represented by characteristic fruits.10 Seward u Spokane and equally doubtful material from Contra has described a large fruit from the supposed Eocene Costa County, Calif., the only Miocene occurrences of of southeastern Nigeria which has the appearance of a Vitis recorded from western North America are two Paliurus but which is not certainly such. species from Florissant, Colo. The genus is consid The Oligocene contains at least three species—one ered by Knowlton to be present in the late Upper from Louisiana represented by very characteristic Cretaceous of New Mexico and Wyomjng, and several leaves and thorny stems and two from southeastern species have been recorded from the early Tertiary of France represented by both leaves and fruit. the western United States, British Columlna, and At least 13 nominal species have been recorded from Alaska. None have been recognized In eastern North the Miocene. These include identifications based upon America in beds earlier than the Pliocene C'trohelle leaves from Alsace, Switzerland, Bohemia, Italy, formation of Alabama. France, Silesia, and two from Florissant, Colo., the last not conclusive in themselves but highly probable Crder PARIETALES in view of the occurrence of typical fruits at the same Family TERWSTROEMIACEAE Miocene horizon in the State of Washington. Miocene Genus GORDONIA species based upon fruits include occurrences in Bohemia and Styria,12 Switzerland,13 and southern Gordonia hesperia Berry Russia. The last, which comes from the Sarmatian Hate 13, Figures 7, 8 stage, is scarcely if at all distinguishable from, the Gordonia he&p&na Berry, Am. Jour. Sci., vol. 18, p. 430, figs. existing Paliurus aculeatus.1* The Pliocene record con- 1, 2, 1929. 10 Berry, E. W., U. 8. Qeol. Survey Prof. Paper 91, p. 279, pi. 71, fig. 4, text fig. Although the specimens of this species from Grand 14, 1916. Coulee are relati ely shorter and wider tl Spokane, the abundance of material from the Spokane Brandon, Vt., but for some reason they are much locality shows that they fall within the limits of vari rarer in the later Tertiary, where we know only this ation of the species. and one other species from the Latah and its equiva It is an interesting fact, already discussed in the lents and a third species from the Miocene Calvert paper above cited, that our northwestern Miocene formation of Virginia. Only two American Miocene contains two species of Gordonia based upon leaves and species based upon leaves are known—the on© men two based upon seeds and that the latter are more tioned above and a second from the Eagle Creek similar to existing Asiatic species than to the existing formation and the Bridge Creek shales c* Chaney in species of southeastern North America. Oregon. Species of Nyssa based upon the stones alone are Order UMBEHALES always of doubtful specific distinctness, and I might Family CORN ACE AE mention a great many so-called species of stones from Genus NYSSA Linne other and very different horizons, both in this country Nyssa hesperia Berry, n. sp. and abroad, which resemble the present species, but Plate 13, Figures 9-11 such comparisons lack any real value. Stones of medium size, prolate spheroidal or slightly POSITION UNCEBTAIN compressed in form, widest medially and about equally Phyllites couleeanns Berry, n. sp. rounded at both ends, with about 10 prominent wide rounded ribs separated by narrow deep sulci. About Plate 13, Figure 12 1.5 centimeters or slightly less in length and about 7.5 This single specimen seems to me so obviously to millimeters in diameter. All the specimens collected represent an abnormal leaf that I have not ventured to are preserved as casts in the clays, and they show attempt a determination. It is elliptical in general various degrees of flattening. The type comes from outline, about 6.5 centimeters long and 4 centi the brickyard exposure of the Latah formation, but meters in maximum width. Apex rounded truncate. they are also not uncommon in the Miocene deposits Base cuneate. Margins entire for their lower two- of Idaho usually referred to the Payette formation. thirds; above with a few subequal prominent teeth. They are very much smaller, more rounded at the ends, Midvein stout and prominent. Secondaries nine or and with fewer ribs than Nyssa magnifica (Knowlton) ten pairs, medium stout; the basal diverge at wide Berry 16 of the Latah formation. They are associated angles approaching 90° and become progressively with the leaves described as Nyssa knowUoni Berry 17 more ascending upward, the angle of divergence in the both in the Latah and in the Payette. tip being about 45°. The lower four or five secondaries The stones of Nyssa are very abundant in the are camptodrome; the remainder are craspedodrome, earlier Tertiary of North America, a great variety ending in the teeth. The tertiaries are ir^istinct. having been described from the Eocene lignites of My belief is that this leaf is an abnormal leaf of " Berry, E. W., TJ. S. Geol. Survey Prof. Paper 164, p. 261,1929. some oak, quite likely the common foam at this out »Idem, p. 261, pi. 59, fig. 7. crop which I have described as Qwercm w TJ. S. GEOLOGICAL STTRVEY PROFESSIONAL PAPER 170 PLATE 11 MIOCENE FLORA FROM GRAND COULEE, WASH. 1. Cone scale of Taxodium dubium (Stemberg) Heer. 4. Hicoria washingtoniana Berry, n. sp., terminal leaflet. 2. Lysichiton washingtonense Berry, n. sp., fragment of a spadix. 5-7. Leaves of Quercus mccanni Berry, n. sp. 3. Juglans egregia Lesquereux, terminal leaflet. TJ. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 12 MIOCENE FLORA FROM GRAND COULEE, WASH. 1. Flower head of Platanus. 4-6. Menispermites latahensis Berry. 2. Ribes fernquisti Berry. 7. Ptelea mtocenica Berry, n. sp. 3. Quercus cognatus Knowlton, fragment with leaf spot fungi. TJ. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 13 11 MIOCENE FLORA FROM GRAND COULEE, WASH. 1-5. Paliurus hesperius Berry. 1, 2, Opposite views of the type; 9-11. Nyssa hesperia Berry, n. sp. 9, 10 from Grand Coulee; 3, side view restored; 4, 5, photographs of smaller specimens, 11 from Spokane. 6. Vtiis bonseri Berry, n. sp., seed, inside view. 12. Phyllites couleeana Berry, n. sp. 7. 8. Oordonia hesperia Berry. 13. Acer merriami Knowlton. PLIOCENE FOSSILS FROM LIMESTONE IN SOUTHERN FLORIDA By WENDELJL, C. MANSFIELD ABSTRACT sandy in places. The type locality of the " Lostmans River limestone " is on the Lostmans River, Cbllier This paper describes the mollusks and echinoids found County, about 15 miles south of station 1/1179, one in limestone dredged from ditches along the Tamiami Trail in southern Florida, in the area mapped as " Lostmans River of the localities at which the fossils described in the limestone (Quaternary)" by Sanford but included in the present paper were collected. Sanford referred th® Pliocene Caloosahatchee formation by Cooke and Mossom on "Lostmans Eiver limestone" to the Pleistocene. the evidence of these fossils as identified by Mansfield. The Cooke and Mossom,8 however, did not adopt this name matrix of the fossils is unlike the typical Caloosahatchee but mapped the area formerly outlined by Sanfottl formation, which is sandy, but the fauna is closely related to that of the upper part of the Caloosahatchee formation for this limestone in part as Miami oolite (jfl^ffc®- and is regarded as a facies of the Caloosahatchee. The fauna cene) and in part as Caloosahatchee marl (Pliocene). shows considerable resemblance to that of the Imperial for The area in which the fossils here described were mation of California but may not be contemporaneous with it. collected is mapped by Cooke and Mossom a? the Caloosahatchee marl, and the area at the type locality INTRODUCTION of the "Lostmans River limestone" as the J^iami The fossils upon which this paper is based were oolite. Cooke and Mossom evidently considered the collected in February, 1927, by C. Wythe Cooke, geolo " Lostmans River limestone " equivalent in age to the gist, of the United States Geological Survey, Stuart Miami oolite. Mossom, then assistant on the Florida Geological Sur • Ball and Harris 4 described the rock at the Lost vey, and W. C. Mansfield. The five collections here mans River as being very hard and compact anc1 con reported upon were obtained along the Tamiami Trail sisting of large masses of Polyzoa more or less com within a northwest-southeast distance of about 34 pletely changed into crystalline limestone, the cavities miles, in Collier and Monroe Counties, Fla. The filled with crystals of calc spar. The only mollusk fossils were embedded in white or gray limestone, here reported from this limestone was a single valve of referred to the Caloosahatchee marl, which had been Chione cancellata* (Linnaeus), a species ranging in age dredged from shallow ditches to form the roadbed of from the Pliocene to the Recent. This specie^ was the Tamiami Trail and which was not observed in found only at one locality (station 1/1177) among place. Cooke and Mossom1 give a brief account of the collections described in the present paper. these collections, referring them to the Pliocene. As I have not seen samples of limestone or organic These collections are of considerable interest because remains from the type locality of the "Losfaaans •they extend the range of Pliocene faunas much farther River limestone," I do not know whether the rock in. south than they had been known before. which the fossils here described were found is the I wish to express my sincere thanks to L. W. Stephen- same as the " Lostmans River limestone " or a differ son and C. Wythe Cooke, of the United States Geo ent limestone, but I am of the opinion that it i^ dif logical Survey, and to Austin H. Clark, of the United ferent. ' States National Museum, for helpful assistance. GEOGRAPHIC OCCURRENCE, MATRIX, AND FAUNAL The photographs for the illustrations of this paper COMPOSITION were made in the laboratory of the United States Geo The following is a brief description of the mate logical Survey by W. O. Hazard, and the prints were rial in which the fossils were embedded, based on retouched by Miss Frances Wieser. the matrix attached to the fossils, and a brief ac count of the kinds of organisms found at each locality. FORMER WORK IN THE AREA Station 1/1176. Tamiami Trail, about 11 miles east by The fossils described in this report were collected north of Marco, Collier County. Dirty-white to gray, rather in the area formerly mapped under the name " Lost hard, porous, nonoolitte limestone with inclusions of clear mans River limestone," proposed by Sanford 2 for a angular quartz grains. The cavities were originally oreupied by the tests of organisms, mainly mollusks. Some of these dark to light crystalline to brittle limestone that is cavities are now partly filled with small, rounded, attached 1 Cooke, C. W., and Mossom, Stuart, Geology of Florida: Florida 8 Cooke, C. W., and Mossom, Stuart, Geology of Florida: Florida Geol. Survey Twentieth Ann. Kept., p. 156, 1929. Geol. Survey Twentieth Ann. Bept, p. 207, 1929. 2 Sanford, Samuel, The topography and geology of southern Florida: 4 Dall, W. H., and Harris, G. D., The Neocene of North America s Florida Geol. Survey Second Ann. Eept.,*p. 222, 1909. U. S. Geol. Survey Bull. 84, p. 100, 44 SHORTEE CONTRIBUTIONS TO GENERAL, GEOLOGY, 1931 limy bodies. The fauna consists of small and large mol- GEOLOGIC OCCURRENCE lusks, bryozoans, and barnacles. To judge from the nature of the matrix, all the organisms came from the same bed. Although the conditions at the localities at which Station 1/1178. Tamiami Trail, about 6 miles west of the the fossils were collected did not afforc1 data, for de crossroads leading to Everglades, Collier County. The matrix is similar to that at station 1/1176. The fauna consists of termining the thickness of the limestone, Sanford 5 large mollusks, bryozoans, foraminifers, and echinoids. The reports that a well drilled at Everglades 4 miles south nature of the matrix indicates that all the fossils came from of station 1/1180 of this paper, passed tl rough 30 feet the same bed. of limestone (presumably the same as the fossil-bear Station 1/1180. Tamiami Trail at Carnestown, 4 miles ing limestone farther north) and 40 fe3t or more of north of Everglades, Collier County. The matrix is similar to that at stations 1/1176 and 1/1178. The fauna consists fine gray sand beneath it. of large mollusks, echinoids, bryozoans, and many small Fossils, either of upper Miocene or Pliocene age, foraminifers. The nature of the matrix indicates that all have been collected by members of the Florida Geo the fossils came from the same bed. logical Survey along the Tamiami Trail 42 miles west Station 1/1177. Tamiami Trail, 5 miles east of Carnes of Miami (about 13 miles east of statior 1/1179) in a town and about 7 miles northeast of Everglades, Collier County. The matrix is similar to that at the localities above beachlike sand, which is overlain by a 3-foot bed of described. The fauna consists of large mollusks, bryozoans, hard yellow limestone containing Ckicne ocmceUata. foraminifers, and echinoderms. The presence of the species The limestone may be a little younger than, the fossil- CMone cancellata (Linnaeus) in this collection may indicate bearing limestone treated in this paper, and the sandy that it came from a stratigraphically higher limestone, as bed may represent the sandy bed benerth 30 feet of this species was not recognized with certainty in the other collections. limestone at Everglades. If these sand" are contem Station 1/1179. Tamiami Trail, 9 miles west of Pinecrest, poraneous, the overlying limestone bed ow beds thicken in sec. 13, T. 54 S., R. 32 E., Monroe County. The matrix is westward. Sufficient information has not been ob mainly similar to that at station 1/1177 but slightly more tained to determine definitely whether there .is one compact and harder. The fauna consists of large mollusks, limestone or more in this area. one species of echinoid, bryozoans, and barnacles. To judge from the nature of the matrix, probably most if not all the 6 Sanford, Samuel, The topography and geology of southern. Blorida: fossils came from the same bed. Florida Geol. Survey Second Ann. Eept., pp. 208, 2.23, 1909. Species and geologic range 1/1176 1/1178 1/1180 1/1177 1/1179 Miocene Pliocene Recent GASTROPODS Terebra dislocata Say______X X X X Fasciolaria sp______-______? X Strombus sp______-______X Turritella, n. sp.? aflf. T. perattenuata Heilprin______X Calyptraea sp______X Crucibulum sp_____--_----______. X PELECYPODS X X X X Glycymeris pectinata (Gmelin)?.. . ______X X Area occidentals Philippi?- _-______-___-.______„___ X X X X X X Ostrea sp., group of O. trigonalis Conrad "-___---______X X X X X X X X X X X X X X X •x X X X X X X X X X X X X X X X X Cardita (Carditamera) sp ______-____-_-_-----__-______-______-__ X X X X X X X X X X X X X X ECHINOIDS Encope macrophora tamiamiensis Mansfield, n. subsp.°______X X . X X X > Same form as in the Pliocene at Alligator Creek, Fla. PLIOCENE FOSSILS PEOM LIMESTONE SOUTHEBK FLOBJDA 45 NATURE OF THE FAUNAS RELATIONSHIP TO OTHER FAUNA&- The faunas include 6 genera of gastropods, 15 genera The faunas from the Tamiami Trail com| •of pelecypods, and 2 genera of echinoids. Aside from closely with those atAHigator Creek, Charlotte pr these, Foraminifera, barnacles, and Bryozoa were ob Fla., which Ball 6 regarded a» younger than tb®.f rona served at a few localities. Among the pelecypods the occurring at Shell Creek, a tributary of Prairie G^ek, scallops and oysters are the most conspicuous forms, Charlotte County, Fla., and assigned to the Pliocene both in the number of species and individuals and in Caloosahatchee marl. the rather large size which some of them attained. The faunas of southern Florida appear to b?. re The echinoid, Encope nia&rophora tanwamiiensis Mans lated to those occurring in. the Imperial field, n. subsp., was found at three localities, and the the marine deposits bordering Carrizo new species Cassid.wlMS everglad-ensis at two localities. (sometimes called Coyote Mountain), The character of the faunas indicates that they lived County, Calif.; in fact, they appear more closely near the shore in comparatively shallow water. related to the Imperial faunas than to any other remote fossil faunas I have seen. AGE OF THE FAUNAS The Imperial formation, proposed by Hanim in Although fossils collected from spoil banks may 1926, was redefined by Woodring 7 and made to em come from more than one bed, nevertheless most of brace the entire series of marine deposits bordering the fossils obtained at these five localities appear to Carrizo Mountain, and to exclude the overlying non- have come from the same bed. However, the occur marine beds. In referring to this formation I have rence of Chione cctxndellata at station 1/1177 may in followed Woodring's definition of it. dicate that it came from a higher bed at that place; The marine beds of the Imperial formation have and the occurrence of the new subspecies Osttea tanm- been called "doubtfully Cretaceous," Miocene, and anmensis monroensis at station 1/1179 may indicate Pliocene. that it came from the higher of two beds at that place. Vaughan,8 relying upon two species of coral, origi The ditches were partly filled with water at the time nally referred them doubtfully to the Cretaeeoua the fossils were collected, and a full section of the Arnold 9 first called them lower Miocene, or simply cut was not revealed. Miocene, but later 10 referred them to the upper Mio The age of the faunas is believed to be Pliocene. cene and correlated them with the Etchegoin forma Although the collections include some forms that were tion of California. The Etchegoin formation is now not found elsewhere and consequently are of little aid considered of Pliocene age. in correlation, a few are like or closely allied to Plio Vaughan, in a later paper,11 concluded that "the cene forms, such as Ostrea^ group of O. trigonaMs, systematic affinities of the fauna of Carrizo Cree^ are Pecten evergladensis, and Encope m^acrophora tcumi- with the Caloosahatchee Pliocene of Florida and the amiensis. On the other hand, one form, Cm^uL-m Pleistocene and living faunas of the Antilles." evergladten'Sis, apparently shows some relationship to a Dickerson 12 states: " Several species appear to be species occurring in the Oligocene. Nevertheless, one identical with forms which are characteristic of the specimen, borrowed for comparison from the Florida Gatun formation, of Miocene age." Geological Survey, collected at Moore Haven, Glades Kew,13 in his studies of the echinoids, referrei the County, Fla., and probably dredged from the canal, beds to the Pliocene. agrees in detail with C. evergladensis. No fossils older 6 DaH, W. H., Contributions to the Tertiary fauna of Florida j Wag than Pliocene have been dredged from the canal in the ner Free Inst. Set Trans., vol. 3, pt, 6, p. 1604, 1903. vicinity of Moore Haven. However, the f aunal f acies 7 Woodring, W. P., Distribution and age of the marine Tertiary de posits of the Colorado Desert: Carnegie Inst. Washington Pa*>, 418, and the apparent stratigraphic relation of the fos- p. 7, 1931. siliferous bed to other formations in southern Florida 8 Vaughan, T. W., The Eocene and lower Oligocene coral famag of suggest strongly a Pliocene rather than an earlier age. the United States: U. S. Geol. Surrey Mon. 39, p. 19, 1900. "Arnold, Ralph, The faunal relations of the Carrizo Creek befls of Some poorly preserved specimens of Foraminifera California [abstract] : Science, new ser., vol. 19, p, 503, 1904; The from stations 1/1177 and 1/1180 were submitted to Tertiary and Quaternary pectens of California: U. B. Geol. Sttrrey Prof. Paper 47, p. 21, 1906. Dr. Joseph A. Oushman for identification. Those "Arnold, Ralph, Paleontology of the Coalinga district, Calif.: TJ. S. from station 1/1177 were unidentifiable, but in the Geol. Surrey Bull. 396, p. 44, 1909. Arnold, Ralph, and Andersen, Robert, Geology and oil resources of the Coalinga district, Calif.: lot from station 1/1180 were found Amphistegina, U. S. Geol. Surrey Bull. 898, p. 189, 1910. lessonii D'Orbigny, Eponoides sp.? (probably the 11 Vaughan, T. W., The reef-coral fauna of Carrfao Cree&, Imperial County, Calif., and its significance: TT. S. Geol. Survey Prof, Pa^et 98, same as one of our living species off the coast), and p. 367, 1917. some internal casts of Qwnquelocylina, and TrUocuh ^Dickerson, R. E., Mollusca of the Carrizo Creek beds and their Caribbean affinities [abstract] : Geol. Soc. America Bull., vol. 29, p. lina. Doctor Cushman states that "these are not 148, 1918. sufficient to place the material with any degree of 18 Kew, W. S. W., Cretaceous and Cenozoic Echinoidea of the Pacific coast of North America: California Univ. Dept, Geology Bull., vol. 12, accuracy, but it is apparently Pliocene or Pleistocene." No. 2, pp. 82, 33, 56, 60, 61, 187, 1920 46 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 Hanna 14 has more recently published a paper in I have not studied the faunas of the Ir*t»rial for which he gives f ormational names to the series of de mation sufficiently to express a definite • opinion as posits about Coyote Mountain, records the faunas, to their age or the relative strat-graphic position of and describes eight new species of mollusks. He con these beds with respect to those lying along the cludes that the age is not greater than lower Pliocene Tamiami Trail in Florida. However, I have ob and is inclined to believe that the greater portion of served certain species in the Florida faur^ts that ap the series is middle and upper Pliocene. The illustra pear to be related to species occurring in the Imperial tions in Hanna's paper were found very helpful for formation and also to species now living in the Gulf comparison with the faunas of southern Florida. of California. This apparent relationship may be a The latest contribution to the paleontology of the Imperial formation has been made by Woodring,18 facies similarity rather than a genetic similarity. who says: Species collected from the Pliocene along the Tamiami Trail that are apparently related to those in The paleontological evidence points to the conclusion that the marine beds of the Colorado Desert are of Miocene age, the Imperial formation and to those now living in and the other two lines of evidence passively support this the Gulf of California are listed below. The species conclusion. There is little on which to base a conclusion named in the middle column were eithe- originally as to what part of the coastal Miocene section is repre sented, but the evidence that is now apparent indicates late described as from the Imperial formation or have Vaqueros age—that is, late lower Miocene. been reported to occur there. Pliocene, southern Florida Imperial formation, California Recent, Gulf of California Ostrea taruiamiensis Mansfield, n. sp______Ostrea heermanni Conrad. Ostrea jacobaea Roehebrune. Pecten tamiamiensis Mansfield, n. sp______Pecten mediacostatus Hanna__. Pecten pittieri collierensis Mansfield, n. subsp___ Pecten subnodosus Sowerby___ Pecten subnodosus Sowerby. Pecten evergladensis Mansfield, n. sp______Pecten deserti Conrad——___. Pecten circularis Sowerby. Thracia (Cyathodonta) tristana Olsson?______Cyathodonta undulata Conrad. Encope macrophora tamiamiensis Mansfield, n. Encope tenuis Kew_ — ______Encope grandis (L. Agassiz). subsp. DESCRIPTIONS OF NEW SPECIES Occurrence: Pliocene. Station 1/1177 (type lo Ostrea tamiamiensis Mansfield, n. sp. cality, 1 valve) ; station 1/1180. (1 valve) ; station 1/1176 (1 valve) ; station 1/1179 (2 valves). Plate 14, Figures 1, 3 The specimens collected at stations 1/1179 and Shell large, rather thin, nearly flat, orbicular, with 1/1176 are much smaller than those collected at sta fluted margins. Exterior surface of holotype partly tions 1/1177 and 1/1180 but have the same general out concealed by matrix but reveals about six rather strong line and appear to belong to the same species. undulating radials. Hinge area rather narrow and Ostrea tamiamiensis monroensis Mansfield n. subsp. furrowed with a rather narrow and shallow channel. Submargins with elongate corrugations. Muscle scar Pltte *4fc if«w:u 2; Plate 15, Mgnres 1-4 orbicular and situated slightly to the left of the center Shell »»Jfafsr thick and heavy, ovate, moderately of left valve. coat«X|fmttt fluted ventral margins in adult speci Dimensions: Holotype, left valve (catalogue No. mens* JBj&e*i0T marked with rath«r sharp, snbspmose 371320, U. S. Nat. Mus.), length, 139 millimeters; ribs separated by de&p and narrow valhys. Hinge height, 131 millimeters. area moderately wide and furrowed with a rather Type locality: Station 1/1177, Tamiami Trail, 5 wide channel. Subamargins with weal" elongated miles east of Carnestown and 7 miles northeast of crenulations. Mttsde sea* prominent and rounded in Everglades, Collier County, Fla. outline. The closest related Recent species appears to be Dimenm PLATES 14-18 51 PLATE 14 FIGURES 1, 3. Ostrea tamiamiensis Mansfield, n. sp., holotype (p. 46). 1. Exterior of left valve. 3. Interior of same valve. FIGURE 2. Ostrea tamiamiensis monroensis Mansfield, n. subsp., paratype, left valve, catalogue No. 371322, U. S. Nat. Mus. (p. 46). FIGURE 4. Turritella sp. aff. Turritella perattenuata Heilprin, catalogue No. 371319, U. S. Nat. Mus., figured specimen. Collected at station 1/1180, Tamiami Trail, Carnestown, 4 miles north of Everglades, Collier County, Fla. 52 TJ. S. GEOLOGICAL SURVEY PROFESSIONAL, PAPER 170 PLATE 14 X3 PLIOCENE FOSSILS FROM LIMESTONE IN SOUTHERN FLORIDA U. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 15 3 4 PLIOCENE FOSSILS FROM LIMESTONE IN SOUTHERN FLORIDA PLATE 15 FIGUBBS 1-4. Ostrea tamiamiensis monroensis Mansfield, n. subsp., cotypes (p. 46). 1. 3. Exterior and interior of right valve. 2. 4. Exterior and interior of left valve. PLATE 16 FIGTTRE 1. Pecten subnodosiis Sowerby. (After Hanna, California Acad. Sci. Proc., 4th ser., vol. 14, No. 18, pi. 25, fig. 6, 1926.> Hanna's figured specimen was collected in a branch of Alverson Canyon, at the base of Coyote Mountain, Imperial Ckranty,. Calif. The photograph is used here for comparison with Figures 3 and 5 of this plate. FIGURE 2. Pecten mediacostotus Hanna. (After Hanna, California Acad. Sci. Proc., 4th ser., vol. 14, No. 18, pi. 24, fig. 2, 1920.) The photograph, taken from the original, is that of the holotype, which was collected from "Alverson Canyon, on the south. side of Coyote Mountain, Imperial County, Calif., in the Pliocene coral reef about midway up the canyon.** is used here for comparison with Figures 4 and 6 on this plate. FIGURES 3, 5. Pecten (Nodipecten) pittieri coUierensis Mansfield, n. subsp. (p. 47). 3. Paratype, right valve. 5. Holotype, left valve. FIGURES 4, 6. Pecten (Lyropecteri) tamiamiensis Mansfield, n. sp., holotype (p. 47). 4. Left valve of specimen. 6. Right valve of specimen. 54 IT. S. GEOLOGICAL SURVEY PLIOCENE FOSSILS FROM LIMESTONE IN SOUTHERN FLORIDA Shows also, for comparison, specimens obtained elsewhere TJ. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 17 PLIOCENE FOSSILS FROM LIMESTONE IN SOUTHERN FLORIDA Shows also, for comparison, specimens obtained elsewhere PLATE 17 FIGURES 1, 2, 4, 5. Pecten (Plagioctenium) evergladensis Mansfield, n. subsp. (p. 47). 1. 4, 5. Holotype, right valve: 1, 4, Exterior and interior of same valve; 5, posterior submargin, showing the nearly smooth area. 2. Paratype, left valve. Collected at station 1/1177, Tamiami Trail, 5 miles east of Carnestown and about 7 miles north east of Everglades, Collier County, Fla. FIGURES 3, 6. Pecten (Lyropecteri) deserti Conrad, left valve, catalogue No. 324564, TJ. S. Nat. Mus. Collected at station 3919 east end of Coyote Mountain, Imperial County, Calif., by Stephen Bowers, 1904. Illustrated for comparison with Figures 1, 2, 4, 5 on this plate. FIGURE 7. Encope grandis (L. Agassiz), upper surface of test, catalogue No. 10013, U. S. Nat. Mus. Photograph of a specimen collected at La Paz, Gulf of California. Illustrated for comparison with Figure 8 on this plate. FIGURE 8. Encope macrophora tamiamiensis Mansfield, n. subsp., holotype, upper surface of test (p. 48). 62508°—32———4 55 PLATE 18 FIGURES 1-10. Cassidulus (Rhynchopygus?) evergladensis Mansfield, n. sp. (p. 48). 1. Right lateral surface of test of smaller cotype. 2. Lower surface of test of smaller cotype. 3. Upper surface of test of smaller cotype. 4. Lower surface of test of paratype, catalogue No. 371330, U. S. Nat. Mus. 5. Diagrammatic view of the preserved part of the apical system, based on the paratype. 6. Left lateral surface of test of paratype. 7. Portion of the anterior ambulacrum on upper surface of paratype. 8. Part of the ambulacral pores around the peristome of paratype. 9. Lower surface of test of larger cotype. 10. Posterior surface of test of larger cotype. 56 U. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 18 8 "^Hi^HHHHHHH^H^HHH^ 10 PLIOCENE FOSSILS FROM LIMESTONE IN SOUTHERN FLORIDA THE GEOLOGIC IMPORTANCE OF THE LIME-SECRETING ALGAE WITH A DESCRIPTION OF A NEW TRAVERTINE-FORMING ORGANISM By MABSHAU, A. HOWE The agency of microscopic algae, especially blue- had been built up by a mixture of blue-green algae, green algae, in depositing lime in calcareous hot of which the predominating kind was /Sefmothrias springs and calcareous streams has long been recog (Inactis) fasdciAa^a (Nasgeli) Gomont, as deter nized. Ferdinand Cohn * was one of the first to inves mined by the eminent authority Gomont. However, tigate the matter in a scientific way, in studying the Gomont 4 describes the trichomes of S. fasofoiti-ata, as deposits.in the famous hot springs of Carlsbad, in 1.4/i to 3/t* in diameter, while Murray's figures, f word Bohemia. ing to the magnifications indicated, show trichomes In America, in 1889, Walter Harvey Weed,2 then a 2.5ju, to 8/A in diameter, Murray mentions Dwl otJm^s member of the United States Geological Survey, pub as intermingled with his jSchizothriw, and it seerxs pos lished a striking report on the formation of travertine sible that some of Ms figures represent Dwkothrios and siliceous sinter by the vegetation of hot springs, rather than Schizothn®. with special reference to the remarkable conditions In 1897 Josephine E. Tilden e described sor^e new found in the Yellowstone National Park. The deposits species of Minnesota algae which live in a calcareous of most of the springs in that region are "siliceous or siliceous matrix. Most of the algae f ormec1 crusts sinter," but the extensive one of the Mammoth Hot of various colors, with a maximum thickness of 1 Springs, covering a total area of about 2 square miles centimeter, on the sides of a large wooden tank on the and having a maximum depth of about 250 feet, con bank of the Mississippi River. New species were de sists chiefly of calcium carbonate or "travertine," scribed in the genera Dichothrix^ Lyngbya,, ScMzo- partly precipitated in a mechanical way, but probably thrisB, and Chaetophom, the last a green alga, the to a much larger degree by the action of microscopic others blue-green. An examination of specimens dis algae. The waters of the Mammoth Hot Springs tributed by Professor Tilden indicates the presence carry a saturated or supersaturated solution of calcium also of the plant that is now referred to Inactis pul- bicarbonate, and much of the lime is deposited by the vinata, Klitzing. It may be the same as the Lyngbya evaporation and cooling of the water. Yet much or vwna, Tilden, the filaments of which are described as most of what geologists call " travertine " at the Mam only 1.9/A in diameter. moth Hot Springs, as has been demonstrated macro- In 1900 John M. Clarke,6 State paleontologist of scopically and microscopically by Weed and others, is New York, published a brief illustrated paper on the due to the action of the abundantly present algae or water biscuit of Squaw Island, Canandaigu% Lake, their chlorophyll in consuming or decomposing the N. Y. Doctor Clark© states: CO3 that is present in the water and thus reducing The north shores of Squaw Island and tne lak^ bottom the amount of calcium bicarbonate that may be held in about it and over its northward sand bar are «OVf*ed with solution. The precipitated lime is a by-product of the flat, whitish calcareous cakes of circular or oval shape, in photosynthesis of the little plants. And the same proc size ranging from a dime to a half dollar. To pick up one ess evidently goes on in both fresh and salt water in of these, well dried on the surface of the island, and break "which calcium bicarbonate is dissolved in much less it in half, seems enough to convince the reflective mind at than saturation proportions. once of their nature and mode of formation. It often con tains as a central nucleus a beach pebble of shale or lime In 1895 George Murray 3 published critical notes on stone, a twig, or a bit of charcoal from some youngster's calcareous pebbles formed by algae, based on material campflre. About this a white or greenish travertine has been from a pond in Michigan separated from Lake Michi deposited in concentric layers, which show themselves with gan by a sand bar. Murray found that these pebbles distinctness. * * * On picking one of the water biscuits 1 Ueber die Algen des Carlsbad Sprudels, mit Riicksicht auf die 4 Monographie des O*elllari6es: Ann. sci. nat., Bot., 7th g«sr., vol. 15, Bildung des Sprudelginters: ScMeslsehe Gesell. vaterl. Cult. Abh., p. 299, 1892. Abt. Naturwiss. u. Medicin, 1862, Heft 2, pp. 35-55. *Bot. Gaz., vol. 23, pp. 95-104, pis. 7-9, 1897. * U. S. Geol. Survey Ninth Ann. Kept., pp. 619-676, pis. 78-87, figs. « New York State MBS. Ball., vol. 8, pp. 105-198, pis. 1&-15, 1900; 52-56, 1889. New York State Mas. 64th Ann. Bept, vol. 8, pp. 19&-198, pis. 1&-15, 8 Phycological Memoirs, pp. 74-77, pi. 19,1895. 1902. 58 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 from the lake bottom, its surface is found to be smooth, slimy, 3. Foraminifera. Recent studies by T. Wayland and often greenish; exposure on the shore bleaches it white. Vaughan and J. A. Gushman have emphasized the The calc-carbonate being dissolved in dilute acid and entirely removed, there remains a soft, spongy organic residuum of geologic importance of this group of microscopic ani precisely the volume of the original biscuit. mals. C. H. Peck, the State botanist, to whom specimens 4. Corals. There are $0ubtiess "true coral reefs"" were submitted, reported that the felted mass was and islands that have been actually built in a pre dominant way by corals, but Funafuti is evidently not made up of several kinds of fresh-water algae and diatoms. He identified one of the species as " prob one of them. ably Isd[c]ti8 f/u/viatilis" That Funafuti is not an isolated example of the In 1903 C. A. Davis,7 after the appearance of three building of reefs by plants rather than by animals is shorter papers with similar titles, published a " con attested by the observations of FinckK Gardiner^ tribution to the natural history of marl," based chiefly Setchell, and others. Gardiner 10 remarlrs that "the on studies of vast deposits of calcium carbonate in importance of the incrusting nullipores in the for Michigan lakes, which form the basis of the cement mation of the reefs of the central Pacific can not be industry in that State. In connection with the origin overestimated." Again,11 in discussing the founda of these extensive accumulations of lime, he ascribes tion of atolls in general, Gardiner says: great importance to the green algal genus Chara, The chief building organism is LitTiotlMmnium, the bathy- though, admitting that blue-green algae are largely metrical zone of which must be limited to a large degree by concerned in forming both the massive beds of lake the extent to which light can penetrate sea water. tufa and concentric calcareous pebbles. In another publication 12 Gardiner says: The importance of certain lime-secreting marine This nullipore [PoroUthon craspedi'um], Fincl'h says, is ac algae in the building of so-called "coral reefs" has tually the reef former at Onoatoa [Gilbert Islands], He saw received increasing attention and emphasis since the no live coral there, but everywhere on the lagoon and ocean, publication by the Royal Society of London, in 1904, face immense masses of this particular nullipore. of a large quarto work on Funafuti,8 which was se That lime-secreting plants rather than corals are lected for this study because it was considered to be sometimes, at least, the dominant reef formers in the a "typical coral " reef or island. Several borings were Indian Ocean as well as in the Pacific is1 attested by made here by members of three successive expeditions. the following observation by Gardiner: 1S The main boring was finally driven down to a depth The reefs of the Chagos are in no way peculiar-save in their of more than 1,100 feet. The cores thus obtained extraordinary paucity of animal life. * * * However, thi& were brought back to England for study and analysis. barrenness is amply compensated for by the enormous quantity A. E. Finckh, who wrote the chapter on the biology of of nullipores (Lithothamnia, etc.), incrusting, massive, mam- reef-forming organisms at Funafuti, groups the va millated, columnar, and branching. The outgrowing seaward edges of the reefs are practically formed by their growths, and rious lime-secreting organisms at Funafuti in order of it is not too much to say that, were it not for the abundance their reef-building importance as follows: and large masses of these organisms, there wouJd be no atolls, 1. Lithothamniwrif by which Finckh means stone- with surface reefs in the Oitagos. like, unsegmented, branched or crustaceous red algae Mme. 0r. A, Weber-van Bosse 14 deseriHs and pub (Rhodophyceae) of the family Corallinaceae. These lishes photographs of extensive LithothoftMmm^ banks. calcareous plants are commonly referred to by geolo near the southwest point of Timor, in the Dutch East gists and zoologists, and occasionally by botanists, as Indies. " nullipores." In 19£1 M&ydr,15 writing of Rose AtoJl, American 2. HcHimeda. This is a genus of lime-secreting Samoa, states that green algae (Chlorophyceae) of the family Codiaceae. It includes several species, of which HaUmeda opwn- There are a few fossil corals, chiefly PodHophw®, embedded in the rock of the atoll rfia and the boulders, but the whole tia appears to be the one that occurs in most abun visible rock of the atoll consists so largely of Lithoth Setehell,16 who has made several visits to the South Foslie 2* have been currently referred to the CaJcaire Sea Islands, largely for the purpose of studying the Carbonifere of Namur, Belgium, but Mme. Lemoine reefs, has in a succinct paper summed up the present has shown that L. belgwum came in reality from the status of our knowledge of the origin of so-called Aptian (Cretaceous) of the French Pyrenees.25 " coral reefs " in part as follows: Fossil organisms of Silurian and Cambrian crigin In closing his article on the building of coral reefs Howe 17 that have been described under the generic name Sole- says: "Much eVidence has accumulated tending to show that nopora have usually been referred to the corallina- the importance of corals in reef building has been much over ceous algae, but in the writer's opinion the Ordovieian estimated and that final honors may yet go to the lime-secreting plants." It seems to me that the final honors can now be type of the genus does not belong in this family, if bestowed, and, without minimizing the contributions of the it is, in fact, an alga. However, there can be no seri corals, there may be added: ous doubt that Urgonian and Jurassic fossils more 1. That without nullipores no "coral reefs" can be or recently placed under /Scdmopora* 26 are true rlgae, would have been formed. closely related to Lithothammtum. ***** 5. That the animal components of the reef of next im Although rhodophyceous algae of the coralline portance after the nullipores are the various incrusting (Lithotham/nktm) group may not be of great antiq species, especially of Polytrema, a genus of Foraminifera. uity, in a geologic sense, algae of a lower group, the Myxophyceae (or Cyanophyceae), more popularly re Later James B. Pollock,18 in a paper on the fring ferred to as the "blue-green algae," were probably ing and fossil reefs of Oahu, states that among the first forms of life. There is superficial The organisms chiefly contributing calcium carbonate to. evidence that many, at least, of the most ancient lime both fossil and fringing reefs are corals and coralline algae. stones, of Cambrian and pre-Cambrian age, were laid The algae contribute more than the corals. The algae are called by the general name of Litfaothamtidum. down by the agency of these blue-green algae and that in mass production of limestone these lowly organisms Calcareous algae of the coralline group occur as well- were much more active then than they are at the pres preserved fossils in limestone rock of Tertiary and ent time. The existence of several kinds of blue-<*reen Quaternary strata. There is evidence 19 that the algae in hot springs 27 shows their adaptation to the Lithothamniwn structure may become gradually ob higher temperatures that doubtless prevailed in the literated, perhaps by the action of percolating water, earlier stages of the development of life on the earth.' resulting in a structureless limestone.20 In America The blue-green algae are always of colonial habit. beautifully preserved fossils of the Lithothamniumi The individuals are of microscopic size, and individu group have been described and figured by the present ality is often poorly defined, but the colonial masses writer 21 from Oligocene and Pleistocene strata of the of the present age are commonly of macroscopic Panama Canal Zone, from the Eocene of St. Bartholo dimensions, and in the geologic past such masses ap mew, the middle Oligocene of Antigua, the upper parently helped to make deposits of lime that aro now Oligocene of Anguilla, and the lower Miocene of Trin conspicuous features of extensive geologic forma idad. Lithothamnium, jurassicum Giimbel 22 has tions. It is to be freely conceded, however, that no been described from the Jurassic of Switzerland, and one of these supposed algal limestones of Cambrian the more or less doubtful Lithothamniwn? ellisiawufm or pre-Cambrian age, when examined microscopically, Howe and Goldman 23 from the Jurassic Ellis forma either decalcified or in ground section, shows any in tion of Montana. Archaeolitkothcwrmium tnarmoreum contestable evidence of an algal nature. In view of (Munier-Chalmas) Foslie and LithophyUum belgi&wn the extreme age of these supposed plants and the 16 Setchell, W. A., Nullipore versus coral in reef formation: Am. extreme delicacy of the gelatinous cell walls of the Philos. Soc. Proc., vol. 65, pp. 136-140, 1926. Myxophyceae, even when more or less calcifiri, it 17 Howe, M. A., Science, new ser., vol. 35, pp. 837-842, 1912. ^Bernice P. Bishop Mus. BulL 55, pp. 1-56, pis. 1-6, 1928. seems unreasonable to expect any preservati9n of their 18 Seward, A. C., Algae as rock-building organisms: Sci. Progress, microscopic cell structure. The firm, always strongly vol. 2, pp. 10-26, 1894. 20 Walther, J., Die gesteinbildenen Kalkalgen des Golfes von Neapel calcified cell walls of the Lithothamnieae, so perfectly und die Entstehjmg structurloser Kalke: Deutsch. Geol. Gesell. —————————————————,———————————.—.———, Zeitschr., Bd. 37, 1885. See also Science, vol. 7, pp. 575, 576, 1886. s* Foslie, M., Remarks on two fossil Lithothamnia: K. Norske a Howe, M. A., On some fossil and recent Lithothamnieae of the Vidensk. Selsk. Skr., 1909, No. 1, pp. 8-5. Panama Canal Zone: TJ. S. Nat. Mus. Bull. 103, pp. 1-13, pis. 1-11, 1919; Tertiary calcareous algae from the islands of St. Bartholomew, 25 Lemoine, Mme. Paul, Contribution 3. I'Stude des Corall'^ac^es Antigua, and Anguilla: Carnegie Inst. Washington Pub. 291, 1919; fossiles, VIII, MeloMsiees de 1'Aptien et de 1'Albien: Soc. gSol. France Two new Lithothairftiieae, calcareous algae, from the lower Miocene of Bull., 4th ser., vol. 25, pp. 5-6, 1925. Trinidad, British West Indies: TJ. S. Nat. Mtis. Proc., vol. 62, art. 7, 26 Pfender, J., Sur la presence d'une Sol6nopore daa« 1'Urgorien d.u pp. 1-3, pis. 1-4, 1922. sudest de la France—Solenopora urgoniana, n. sp.: Soc. g&tL France 38 Giimbel, C. W., Die sogenannten Nulliporen: K. bayerisch. Akad. Bull., 4th ser., vol. 30, pp. 101-105, pi. 8, 1930; Leg Sol&xopeN-es du Wiss., Math.-phys. Klasse, Abh., volf 11, Abt. 1, p. 43, pi. 2, figs. 9a, Jurassique supSrieur en Basse-Provence calcaire et celles da Bassin 9b, 1871. de Paris: Idem, pp. 149-164, pis. 16-19. 35 Howe, M. A., and Goldman, M. I., Am. Jour. Sci., 5th ser., vol. 10, 187 Setchell, W. A,, The upper temperature limits of life: Fcience, pp. 314-324, figs. 1-11, 1925. new ser., vol. 17, pp. 834-»Sf, 1903. 60 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1931 preserved in various Tertiary and Quaternary strata, In 1914 G. R. Wieland,*4 accepting tibe various are in a very different category. In the calcareous species of Cn/pt&zoon as algae, refers to the pre-Com- travertine or tufa now being laid down by various brian, Cambrian, and Ordovician ages as character- blue-green algae in lakes and streams in the United ized by the " reign of algae " and adds: States, it is commonly difficult to demonstrate and Nor does it even seem too much to say tfci»t no dominant identify the contributing organisms except in the organisms of later ages, whether plant or animal, ever ex superficial layers. Why should one expect their deli ceeded the Paleozoic seaweeds or left a bulkier record. cate structure to persist for millions of years? Nev A little later in 1914 Charles D. Walcott, dis ertheless, one who is accustomed to see and to handle tinguished Secretary of the Smithsonian Institution,, the- algae of the present day may feel convinced from published his striking paper on pre-Canabrian Algon their macroscopic characters that certain laminated kian algal flora,35 in which he takes the ground that ancient limestones were laid down by algae, even while the extensive (iionmarine ?) magnesian limestones of admitting more or less subconsciously the possibility Algonkian age (chiefly in the Belt Mountains of Mon of being deceived. tana) were laid down by algae of the blue-green group^ In Great Britain the writings of A. C. Seward 28 much as deposits of lime are now being made, on a and E. J. Garwood 29 have emphasized the geologic smaller scale, by blue-green algae in fresh-water importance of the algae, though Seward is dubious as streams, ponds, and lakes in various parts of the to the algal nature of so-called organisms referred to United States. Walcott gave several nev* generic and the genus Cryptozoon and of the Algonkian lime specific names to these supposed fossil algae, although stones described and figured by Walcott. The liter there seems to be scarcely any definitely conclusive ature relating to the geologic significance of the algae evidence in their microscopic structure tha^ these for is becoming extensive, and it is not the writer's pur mations are due to algae at all. Howevf*, from their pose to attempt any complete review of it at this time. general macroscopic characteristics it seems proba A valuable bibliography of the subject, even though ble to the present writer that some, peri ^ps most, of notably incomplete in its American references, is given these new generic names were applied to real algae by J. Pia.30 or to their very ancient forerunners. The magnitude In the United States, in 1913, Eliot Blackwelder 31 of some of these limestone deposits is indicated by made a notable contribution to the subject, in which Walcott's remark that " in the Camp Creek: section of he published photographs showing a remarkable re Montana Collenia, was found to range up through semblance of deposits of Ordovician dolomite to mod 2,500 feet (760 meters) of strata." 36 T>-re are also ern reefs of calcareous algae of the Lithothammwm extensive deposits of Algonkian limestones in Arizona, group. The probability of calcareous algae having in the Grand Canyon of the Colorado. The study of something to do with the formation of magnesian the supposed fossil algae of that region, b^gun by Wal limestone and dolomite is heightened by chemical cott and by Dawson, is being continued by David analyses 32 of various lime-secreting marine organ White.37 isms, showing high percentages of magnesium car E. S. Moore 38 has directed attention to massive bonate in the lithothamnioid algae, whereas the madre- strata of ancient presumably algal limestones, more porian corals are notably deficient in magnesium. A or less sUicified, on the Belcher Islands, Hudson Bay,, similar inference may be drawn from the biologic and and the adjacent mainland. These strata- attain a* chemical analyses of the borings at Funafuti, to which thickness of 428 feet and are considered to be of pre- reference has already been made. Clarke and Cambrian age. The contributing organism shows con Wheeler 83 have already stated that centric layers, somewhat as in the (Jryptozoon proli- In short, all the evidence goes to prove the importance of fet^wm from the Cambrian of Saratoga County, N. Y., the algae as limestone builders and the subordinate character and the OoUenia, freywens from the pre-Cambrian of the corals. This importance is now fully recognized by stu of Meagher, Mont. Professor Moore has found S9 dents of marine limestones and by paleontologists generally. similar calcareous concretions in pre-Cambrian rock 28 Op. cit.; Fossil plants, pp. 122, 123, 1898; The earlier records of from the vicinity of Port Arthur, Ontario. plant life: Geol. Soc. London Proc., vol. 79, pp. lxvi~civ, 1923; Plant life through the ages, 1931. M Further notes on Osarttan seaweeds and oolites: Ana. Mas, Nat. 20 On the Important part played by calcareous algae at certain Hist. Ball., vol. 33, pp. 237-~20p, Apr. 14, 1014. geological horizons: Geol. Mag., new ser., dec. 5, vol. 10, pp. 440-446, * SmithsOBiaa Misc. ColL, Tol. 64, pp. 77-156, $& 4-23, July 22, 490-498, 545'-553, 1913; Nature, vol. 92, pp. 111-121, Sept. 25, 1913. 1914. 80 Geologisches Alter und geographische Verbreitung der wichtigsten **Ideitf, p. 98. Algengrupper: Oester. Bot. Zeitung, Band 73, pp. 174-190, 1924. * Study of the fossil floras of the Graitd Canyon Arizona: Car 31 Origin of the Bighorn dolomite of Wyoming: Geol. Soc. America negie lust. Wasaingto» Teartook NOB. 26, 27, 28 and 29; Algal Bull., vol. 24, pp. 607-624, pis. 28-35, 1913. deposits of Unkar Proterojsole age in the Grand Canyon, Arizona: 38 See Clarke, F. W., and Wheeler, W. C., The inorganic constituents Nat. Acad. Sci. Proc., vol., 14, No. 7, pp. 597-W, J028. of marine invertebrates: TJ. S. Geol. Survey Prof. Paper 102, 1917. 38 The iron formation on Belcher Islands, Hudson Bay» with special Pages 44-50 are devoted to analyses of calcareous Rhodophyceae and reference to its origin and its associated algal limestones 40 U. S. Geol. Survey Prof. Paper 154, pp. 203-223, pis. 28-48, 1929. *» Concretions In streams formed by the agency of W«e-gre?a algae- **• Pre-Cambrian Algonkian algal flora: Smithsonian Misc. Coll., vol. and related plants: Am. Philos. Soe. Proc., vol. 54, pp. 240-r1^, flgs. 64, p. 86, pi. 4, flgs. 3, 4, 1914. 1-2, 1915. ** Algae reefs and oolites of the Green River formation : U. S. Geol. ** Michigan Acad. Sci. Ann. Sept., vol. 20, pp. 24T-260, pis. 16, IT* Survey Prof. Paper 154, pp. 203-223, pis. 28-48, 1929. 1918. 62 SHOBTEE CONTEIBUTIONS TO GENERAL, GEOLOGY, 1931 miles above Harpers Ferry, W. Va. He brought also, in place. An extreme deficiency of rainfall during from more rapidly flowing water in the same stream, the preceding six months had left the stream very more extensive rocklike deposits of lime, of the general low, and the calcareous pebbles in the s'ower parts Mnd commonly known to geologists as "travertine." and the expansive calcareous travertine in the .more The first microscopic examinations of ground sections rapid parts were readily accessible. The^e had been and of decalcified preparations showed a mixture of a rain (about one-third of an inch in. Washington) minute plants—diatoms, unicellular Chlorophyceae, the afternoon and evening before, and the stream unicellular and filamentous Myxophyceae (Cyanophy- was higher than the former low levels, though the ceae), and possibly bacteria—and, in parts exposed to water was still clear. A sample of the water, thus rapid water, the filamentous prothallus of a Lemanea. presumably diluted from the concentration of the In parts of the deposit there was a dominance of a preceding day, was taken to Washington by Mr. minute filamentous blue-green alga, with colored parts White for analysis, which showed the following con (trichomes) only I/* or a little more in width. These stituents, in parts per million: apparently belong to the genus Inactis (a section of COS ______0 Schizothrim of some authors) and to the species HCO3______- 237 Inactis pulvinata Kiitzing, originally described from Iron______—__———————— . 1 Mn______. 7 Germany in 1849, since reported from cataracts in Ca ______—__—__——^ 06 North America, and known to form hard deposits Total hardness-—__———_~———————— 255 of lime. Mixed with the more or less erect filaments In the rapids, especially in the shaded recesses, the of the Inactis and in places predominating were much superficial crust is conspicuously black or r.t least dark coarser filaments (trichomes 6/* to T/* in diameter) with or rust-colored. Mr. White states (in a letter) that firm, rigid sheaths; these filaments appear to be refer the lime is here associated with manganiferous iron able to Lyngbya martensiana calcarea Tilden, orig oxides. Sections show a laminated strvTture, with inally described from Minnesota. There are, how dark layers occurring at irregular intervals, and Mr. ever, wide areas of this Furnace Creek deposit that White suggests that the deposits of iron an4 manga show no traces of either the Lyngbya or the Inactis, nese accompany the greater concentration of these and further studies indicated that very numerous metals in the water in seasons of drougHj, the year minute particles which'had at first been passed over 1930, in which the deposit was very notable, being one as bacteria or granules of an inorganic nature often in which the annual rainfall in the Washington region showed in mass traces of a light blue-green or yellow was only about half the normal. ish-green color. The conviction grew that they were In spite of the differences in appearance between the representatives of the Myxophyceae, smaller, perhaps, olive-brown, ash-colored, or subfascour concentric than any previously known, and that they were the pebbles of the moderately Class MYXOPHYCEAE the young very jjate M«e-greiB% losing color with forming a hard laminate crust 1 millimeter to a few or Family CHROOCOCCACEAE many centimeters in thickness, the surface sordid, oli Genus LITHOMYXA, n. geia.45 vaceous, ash-colored, fuscous, or black, nearly smooth, Cells subglobose, ovoid, or short cylindric, very mi verrucose, f oveolate, scrobieulate, irregularly nodose or nute, associated in great numbers in an extended la$er, clivulose, or coarsely mammillate. precipitating lime and forming a rocklike crust. Cell In a stream known as Furnace Creek, a tributary membranes soft, very inconspicuous, confluent. Cell of the Potomac Eiver, 1% miles above Harpers Ferry, division apparently in one direction; cells solitary, in W. Va. Type in the herbarium of the Ke^ York twos, irregularly in fours, or often few or many con Botanical Garden, collected by David White, Charles globate. Chromatophore not definite; chlorophyll B. Bead, and Marshall A. Howe, December 7, 1930. very little, in dark places perhaps wanting. The technical type is considered to be one of the con The genus shows points of contact with Aphano- centric pebbles found on the bed of the str«sam in thece, Aphanocapsa, Synechococcus, Synechocystis^ rather quiet water. The more extensive and more Oncobyrsa, and Chlor&gloea. Perhaps it may be massive, usually black or fuscous crusts found in the placed provisionally between Oncobyrsa, 4e and Ohloro- more rapidly moving water may be considered as de gloea>, from both of which it differs in the essential posited by the form femfera, if a distinctive name is lack of radial arrangement of its cells. The type and required. This appears to differ from the type only only known species is described below: in color (which may be looked upon as a sort of stain) and in its ability to precipitate considerable quantities Lithomyxa calcigena Howe, n. sp. of iron and manganese, which may be conditioned on its occurrence in rapidly moying, well-aerated, and Plates 19-23 perhaps well-shaded water. The same organism in Cells mostly 0.4/t to 1.5/» long and 0.8/t to I/* wide, different surroundings appears to have different physi before division usually about twice as long as wide, ological or chemical effects. In ground vertical or radiovertical sections the margin (surface) sometimes 46 lAthomysca, gen. nov. (fam. Chroococcacearum, class. Myxophyce^i- shows 2, 3, or 4 cells in an anticlinal row, but in gen rum). Cellulae subglobosae, ovoideae, Tel brevi-cylindrieae, mimitissimae. Jn eral the cells are without order, their lon§^r axes strato expanse numerosiggimae confertae, calce Induratae, crugtajn lying in any direction. lithoideant efflcienteg. Membranae mollissimae, valde incongpicuae, confluenteg. Cellularum divisio per speclem In directionem ad unata In the quiet water the L$£homa/3&ffi is often associated dimensionem, cellullg solitariis, binig, irregulariter quaternig, gaepe with Diatomaceae, ProtoeoGeaceae, and Chr *T Equivalent to 0.17 per cent PeO. The iron is probably in the *The aboye paper, in a condensed form and illustrated by lantern ferrous condition, but the differentiation of ferrous and ferric Iron Is slides, was presented at a meeting of the National Academy of Sciences uncertain in the presence of organic matter.—R. C. Wells. held at Washington April 28, 1931. IT. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 19 A. CALCAREOUS CONCRETIONS FORMED CHIEFLY BY LITHOMYXA CALCIGENA From bottom of Furnace Creek, in rather quiet water, near Harpers Ferry, W. Va.; collected by White, Howe, and Read December 7, 1930. A decalcified preparation, made from the superficial crust of the bisecte_d pebble shown in the upper left-hand corner and preserved in the herbarium of the New York Botanical Garden, is specified as the technical type of Lithomyxa calcigena. B. A PORTION OF A GROUND SECTION OF ONE OF THE PEBBLES FROM FURNACE CREEK Showing, especially in the lower central region, outlines of the Lithomyxa cells, with incrusting lime; at the upper margin (surface) the cells sometimes appear to be in rows of two, three, or four. U. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 20 . A PORTION OF A GROUND VERTICAL SECTION OF THE BLACK CRUST ILLUS TRATED IN E Showing outlines of the calcified Lifhomyxa cells. B. DARK OR BLACK CRUST, FORMED CHIEFLY BY LITHOMYXA CALCIGENA FORM FERRIFERA, IN SHADED OR PARTLY SHADED PLACES IN RAPIDLY MOVING WATER, FURNACE CREEK, W. VA. Collected by White, Howe, and Read December 7, 19_30. The darkening of the crust is apparently due to the presence of iron and manganese. The upper view indicates the readiness with which the superficial dark crust (a loose fragment here dislocated) separates from the underlying white crust, which also has been laid down by the Lithomyxa. TJ. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 21 CALCAREOUS TRAVERTINE FORMED CHIEFLY BY LITHOMYXA CALCIGENA FORM FERRIFERA, IN MORE OR LESS SHADED PLACES IN RAPIDLY MOVING WATER, FURNACE CREEK, W. VA. Collected by White, Howe, and Read December 7, 1930. U. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 22 A. LITHOMYXA CALCIGENA, DECALCIFIED, MORE OR LESS EMBEDDED IN COLLOIDAL JELLY, FROM SURFACE LAYER OF A CALCAREOUS PEBBLE, FURNACE CREEK, W. VA. • Collected by White, Howe, and Read December 7, 1930. £v.ft-£ B. A SIMILAR PREPARATION OF LITHOMYXA CALCIGENA FORM FERRIFERA, FROM THE BLACK CRUST TJ. S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 170 PLATE 23 A. SPECIMEN OF TRAVERTINE The gray travertine at the left is made chiefly by two filamentous blue-green algae, Lyngbya martensiana calcarea and Inadis pulvinata; the black travertine at the right was laid down chiefly by the more minute unicellular organism, Litkomyxa calcigena. B. A GROUND SECTION AT THE LINE OF JUNCTURE OF THE GRAY TRAVERTINE AND THE BLACK The Lyngbya and Inadis form the looser and (in section) flabellate crusts at the left. The Liihomyxa forms the more compact and homogeneous crust at the right. PLATES 19-23 INDEX A Page !»*§« Acantboceras (Prionotropis) allaudi..____.__.______11,17 Beny, Edward Wilber, A Miocene flora tram Grand Coulee, Wash. ____ 31-42 Acei fruit... —————.————————.——————————————————„ 33,34 Betula heteromorpha,—_____..————___———-...__——__ 33, S4 merriamL.,____.______33,34,39 largei. Acknowledgments for aid-....______9,43 Bonser, T. A., quoted______. 31 Admiralty Island, Alaska, evidence of pre-Wisconsin glaciation on....___ 8 Bridge Creek, flora of______. 33 Alaska, existing glaciers in—...——.—__..__.._....__„_____ 1-2 Brooks Range, Alaska, glaciers of.. 2,3-4 former glacial advances in..—______.__ 2-4 Buchiceras nardini- __——..... 9 glaciation in, studies of..-..——..——.____.______1 position of 100 and 50 fathom depth contours in places along southern coast of, map showing______.. pi. 2 California, Miocene floras of, comparison of, with flora of Grand pre-Wisconsin glaciation in, evidence of...______.. 6-8 Wash...—————.——.———..______...______33 map showing__—...——_~__.______.__.______pi. 1 Calyptraea sp———__————___.______44 summary of known facts concerning______,______7-8 Capps, Stephen R., Glaciation in Alaska______1-8 relations between climate and glaciation in. _____.______8 Cardita (Carditamera) sp.-..-——______44 Wisconsin glaciers of, map showing areas covered by..______pi. 1 Cardium sp__.______.______44 map showing lines of flow of.———..——_.__..___.__..__ pi 2 Carpites boraginoides. ______r...... 33,34 Alaska Range, glaciers in.——..„.._—_...._.__..__..._____ 2,3 Algae, lime-secreting, geologic work of..__..______59-61 ....————.———.—....——....——..——.__ 33, 34 .... — .—...... ———...... —————..———_„.—__ 33, 34 Alstadenites..——.—————————.——..——„——.—...—__.__ 14,16 Cassidulus (Pyjoraynehus) alabamensis.______48 Ammonites alstadenensis--__...______9 (Rhynchopygus?) evergladensis——.„______.___ 44,46,4f, pi. 18 dentato-carinatus__.._____..______9,10,15 Castanea castaneaefolia_—„•————______33,34 fleuriausianus..___.______14-15 Cebatha heteromorpha__.______32,33,34,37 haberfellneri_——...——..——...... ______9 multiformis^----___._„_.„...______,______37 neptuni..——.————————————..——_—_..__._____ 9 Chaetophora__———————————————_——___————_____ 67 paeon...—....——.——..——-..--.-..__.__..._._____ 9 Chara______.__...__—————_____.______61 petrocoriensis....—.——.-——-...__..______9 Chatham Straits, Alaska, origin of__—______.______.. 2-3 rhotomagensis_.._—_—_..__.______10 Chichagof Island, Alaska, evidence of pre-Wisconsin gladation on_____ 8 Amphistegina lessonii.__..__—_..______.______45 Chione cancellata..._—————————-——-_____—....____ 43, 44,45 Anomia simplex._————————————...—_...... ___.____ 44 Aphanocapsa——..————.——————„——_—.„—__—_„__ 61,63 intapurpurea.———————————————————————————_-__ 44 Chlorellopsis cofoniata.—————————————————————______61 Aphanothece—__—————-—————_—_.__—__—__.__ 63 Chlorogloea.__————1——————_——..———.....—..._____ 63 Area (Anadara) sp_.__—__—„.„_____—____.______44 Cissampelos dubiosa..___._.____.„__.___..____f...... 37 Archaeolithothamnium marmoreum ....__—______69 Clarke, F. W., and Wheeler, W. C., quoted______.______60 Atolls, building of, by lime-secreting plants_____._____._____ 58-59 Clarke, J. M., quoted...————————————————————:„..___ 57-68 B Collenia frequens.——————————————————————————————__. 60 Baculites codyensis.———— ..„——.——..——...——.———.—_..__ 18 Coral reefs, work of lime-secreting algae in building...... ———....___«,_ 68-59 Barroisiceras Grossouvre, taxonomic history of..______9-11 Crucibulum sp—————————————————————————————————..... 44 Karroisiceras allaudi———————....—...... __——..—__._____ 12,14 Cryptozoon, geologic importance of..—————...__...————_____ 60 alstadenense._—..„_—...——..——„..__..._.____ 11,12,14,16,18 Cryptozoon proMferum__—.————...... _____————_____ 60 boisselleri__.——_———..„—__._....____._.___ 9,10,13 Cyathodonta undulata———————————————————————.————_ 4ft brancoi____—__.__.______._ 10,11,14 armatum______10,13,14 D mite...————————— r-————————-—-....— 10,13,14 Dichothrix.-_.....—__.....——....._———.——..____...... 67 byzacenicum————.—————————.———————.——.—___ 13,14,19 Divaricellasp-.———————————————————————————————— 44 castellense------___ 13,14,17,19,25, pL 6 £ dartoni—.._———-———————————.—__ 12,14,16,25,26, pis. 6,7 Eagle formation, flora of———————————————————————————— . 33 dentatocarinatum____._.____ 9,10,11,12,14,15,19,22,23,24, pis. 3,4,6 Ellensburg formation, flora of.————————————————————————— 33 desmoulinsi.. —————.—————..—_...__.__.______10,13,17 Encope grandis_——————————————————————-———— 46,4f,pL 17 forresterL—— „..—...... ——....———...... 12,14,17,24, pi. 5 macrophora tamiamiensis.—————————————————— 44,45,48-49, pi. 17 haberfellneri__..__..._...... __._.______9,10,11,13,14,16 tenuis____.—————————————————————————————————— 46 alstadenensis.__.___.______.______9,10 Eponoides sp.?—-——————————————————————————————— 45 byzacenicum.__.___.______.______10 Euonymus knowltoni__————————————————————————__ 33,34 desmoulinsi.---_—__.______.______9,10 harlei-.—_————.__._.._____._.___.___... 9,10,11 F nicklesi..__..._—______..+______.__ 11 Fasciolaria sp. _————————————————————————————————— 44 harlei—.—————————————.—....————.—.——. 13,14,19 FioismterglaciaMs.--—-___.__.„.——_._...... ————___ 88,34,37 haueri...... ————————————————————— 10,11,14 washingtonensis————————.———————————————————— 3f. 34,37 hobsoni. __.______._... 12,16,18-19,28,29, pis. 9,10 Florida, southern, geologic work in—————————————————————— 43 hyatti————...—...... -—...—...... __———...... 10 southern, Pliocene faunas of———————————————————————— 43-66 inerme...———.————.——————_.__„__.______13 Florissant, Colo., flora of_.——————————————————————————— 33 knighteni..——.————————————_..._..__.______13 Forresteria—..——————————————.-—---——— 14,17-19 nardini_.—————————————————.—_...... 12,14 Funafuti, studies of reef-forming organisms at————————————————— 68 neptuni...———————————.—————————...———.—..... 11,12,14 Furnace Creek, W. Va., chemical analysis of water of __——————..._ 62 nicklesi————.———————————.——..—...... —... 9,10,11,12,14 new travertine-fanning organism from—————————————61-64, pis 19-23 paeon—————.—————————————————.——————_—.. 12,14 petrocoriense.-.-——————-——..—__.______11,12,14,15 G romieuxi.______10,13,14 Gardiner, J. 8., quoted————————————————————————————— 68 sequens. ______.______9,10,13 Oastrochaena sp_—————————————————————————————— 44 sevierense______.______....__.._..... 12,14,16-17,18,23, pL 4 Glaciers in Alaska, existing.————————————————.—————————— 1-2 siskiyouense—....—.————————__.______13 existing, map showing largest——————————————————————— pi. 1 sp.————————————.——————.——-—.—.———„—_ 19,25, pi. 6 formation of, during former stages of ice expansion.——————————— 2 stantoni—————...... 12,14,16,17-18,19,26,27,28, pis. 7,8,9 outlets for former, from coastal mountains————————————————— 3 texanum______10 Gloeocapsa_____....—.—————————————————————————— 61,68 tunetanum.._____——_..._.______10,13 | Gloeotheee...__—————————————————————————————— «1 67 68 INDEX Page Glycymeris americana——————————————————_..——_____ 44 Paunella....———..———————————————————————————————— 61 pectinata______44 Payette formation, flora of——————————————————————————— 33 Glyptostrobus europaeus_____..____.____:______32,33,34 Pecten circularis____————————————————————————————— 46,48 Oordonia hesperia___--__-_._____.______. 33,34,41-42, pi. 13 gibbus gibbus.__...——.—————————————————————.—— 48 Grand Coulee, Wash., Miocene flora from, age of____-...______._ 32 (Lyropecten) desert!__-_————————————————————-- «fe pi. 17 Miocene flora from, compared with Miocene floras from other localities_ 33 tamiamiensis___—__———————————————— 44, 46, 47, pi. 19 features of___.______.______31-42 mediacostatus-. __—————————————————————————— 48, 47, J}L ~ H Gryphaeaaff. G.aucella..--____.--.______.--._.____.___ 16 mendenhalli_____——__————————————————————————— 48 Gulf of California, living fauna of, compared with Pliocene fauna of southern (Nodipecten) pittieri collierensis-—.————.—————.—- 44,46, 47, pi. W Florida——————.—,————.————.....—.. 46 (Pecten) sp.____———.——————————————————————— 44 (Plagioctenium) comparilis..——————————————————————— 48 H evergladensis___—_———.———————————— 44,48,48,47, pL 17 Halimeda opuntia___.______58 subnodosus____——————————————————-————————— 46, pi.. 16 Harleites-—. ——______.______.______._____ 14,19 Phyllites amplexicaulis_..__———-——————————————————— 33,34 Hicoria washingtoniana.. ______32,33,34, pi. 11 couleeanus._____-___———-—————————————— 3§,S4,42, pi. 13 Howe, Marshall A., The geologic importance of the lime-secreting algae, with Pinna sp.-..———.———————————————————————-———————— 44 a description of a new travertine-forming organism. ______57-65 Placenticeras pseudoplacenta..———————————————————————— 18 Platanus aspera- __—————————————————————————————— 33,34 dissecta.---____-—-—-———-——-———————————————-—— 33,34 Imperial formation, California, faunas of, relations of.______45,46 flower head,—__.——.——-——....——;————————— 83,33,84,37, pi. 12 Inactis pulvinata..-——____.______57,62,63,64 Plicatula marginata. ————————————————————————————.— 44 Inoceramus aff. I. deformis..-__..______.._ 15,16 Pliocene faunas from southern Florida, age of.———————————————— 45 aff. I. erectus__.-.-.___..___.______18 composition of._——— —————————————————————————— — 43-44,45 aff. I. fragilis.._.-.-______18 general features of...———— ——— —————— ———————————— 43-56 deformis______.______17 geographic occurrence of—————————————————————————— 43-44 fragilis..——_——————...... __——._.._„___._.__ 17 geologic occurrence of——————————————————————————— 44 stantoni.—__.——....-„...____„______18 nature of..—————————————————————————-——-————— 45 umbonatus____—____..______._____ 18 relationship of, to other faunas.—————————————————————— 45-46 Inodennalamellosum..--______63 Pocillophora__—__————————————————————————————— 58 Isa[c]tis fluviatilis._—___——______58 Pollock, James B., quoted——.————————————————:———————— 59 J Polytrema__ — ————— -—————————————————————————— 59 Juglansegregia..-.————————————————————__— 32, 33,34,35, pi. 11 Populus arctica———————————————— ———————— ——————— 38 bud scales---___-——-——-———————————————————.—— 33,34 L fairit———————————————————————————— 37 Latah formation, flora of..__——______33 heeri...———————————————_—-———————— 35 Lauras similis____——____. ______33,34 heteromorpha.__——--—————————————————————————- 37 Lemanea———_———.—————_—...______62 lesquereuxi.——.——-—————.——-—-—-———-—————— 33,34,35 Libocedrus praedecurrens.. ______33,34 lindgreni..————--—————— ———.——————.——. 33,34 Lime-secreting algae, geologic work of...——______.______59-61 washingtonensis——..— —————————————————— -————————— 33,34 Liquidambar californicum______r ______• 39 Porolithoncraspedium.-.————————-——————————.————————— 58 fruit.--—————————————————..-.——————..... 33,34,38-39 Prince of Wales Island, Alaska, evidence of pre-Wisconsin gkciation on..._ 8 pachyphyllum.———_———___——______.______.. 39 Prionocycles macombi-————————————————————————————— 17 Lithomyxa Howe, n. gen___,______.______._ 63 wyomingensis.-— ———————————————————-———————— 17 calcigena Howe, n. sp.______-______.__ 63-64, pis. 19-23 Prionotropis hyatti————————————————————————————————— 17 Lithophyllumbelgicum.______.______.. 59 Prunus rusti--..————-————————————————————————————— 33,34 Lithothamnium..______.______.______58,59,60 Ptelea miocenica. - ____-___——————————————— 82,33,34, 39, pi. 12 ? ellisianum Howe and Goldman______.. 59 trifoliata—__.....-——-———-—-———————————-———— 39 jurassicum Giimbel.____..-.__—______59 Lyngbya——————————————————-————————.__——____ 57,62,63 martensiana calcarea..._.--.___——______62,63,64 nana------___—____..-._——___—.______57 Quercus acapulcensis—————————————————————————————— 36 Lynn Canal, Alaska, origin of.—.__———__ __.______2-3 acorns and cupules.. ————— ———————————————————————— 33,34 Lysichiton washingtonense______32, 33, 34, 35, pi. 11 chaneyi_—————————————————————————————————— 36 chartacea.—————————————————————————————————— 36 M chihuaiiuensis.-———————————— ———————— ———————— 37 Mansfield, Wendell C., Pliocene fossils from limestone in southern Florida.. 43-56 elaraenste.—————————————————————————————— 36 Mascall formation, flora of______33 eognftta___._>.—————._,—————————————— 33,34 Mayor, A. G., quoted___.______.______.____:___. 58 homiaoa--______36 Menispermites latahensis._____.______...____ 33, 34, 38, pi. 12 hypeteBea—.__———.—-—.———————.—-—-————— 36 Metis magnoliana._...______.______,______44 lecomteana————————————————————————,———————— 37 Microcoleus paludosus...____.___.______.__•______61 martensiana—..-———*.———————————————————————— 36 Mortoniceras shoshonense______-______.______18 mccannl—.-,————————————————,.. 8^348ft, 42,pi. 11 merriaunl—,——————,———————,.—————————————— N Nyssa hesperia.-—------—————.——.———.——....———. 33, 34, 42, pi. 13 obscura knowltoni.__——-._———___——______42 oteoides. 37 magnifica——————.——————-————————————————...... 33,34,42 — 33,34 O phellos. __ — ——— — ...... ———— . —— . — — — — ...... 36 praenigra. —— .. —————————————— r ———————————————— 36 Oncobyrsa. — ..——————. ——.—.....______._.___..... 63 prinopsis ___ .. —————————————————————————————— 36 fluviatilis- .———————————————...... 63 pseudolyrata. __ — "... - ———————————— - ——————————— «. 83, 34. Ostrea heermanni. .. — - — - — .—.—------_....._...... _ 46 repanda __ . __ — — . — - ——————————————————— -,-, —— 37 jacobaea .———— ——— — ——— . — ——— — ——— — — —— . 46 simulata—— -.—————————————- — .—————^^,^38,34,36 lugubris _————— ———— —— ——————.————— ——— _ 17 spokanensis.-.. ————— ,. ———————————, ——————————— 36 sculpturata______. 44,47 transmontana. ______., ______.. ______- __ .__. 36 sp., group of O. trigonalis_—_———______44,45 treteasii.---.-—— .—-,.—— ^-——————————————— 33, 34, 37 tamiamiensis_——_————__.——_____...."_____ 44, 46, pl.14 viminea ______i ———— , —————————————————————— 36 monroensis_——_—..._____.______44, 46, pis. 14,15 trigonalis, group of.._...——____.______.______44,45 E Reeside, John B., jr., The Upper Cretaceous ammonite gerns Barroisiceras Paliurus aculeatus ______40,41 in the United State.... .—————————— .— — — — - 9-29 hesperius.—— ...... _ ...... _ .. __ ———— ...... 33, 34, 39-41, pi. 13 Ribes femtuMJ.....—l—— „-————————————— 83,3438,51.12 orientalis— _ __ — _ . __ . _ ___ . ______40,41 Baddy, H. Jostin, quoted—. , ———————————————————————— 61 ramosissimus..— —— __ — ... ______, _____ 40 RusseH Qfeaster, Alaska, nMatteum extent of. ——————————————— 6 OTDEX 8 Page Terebra dislocata..——„.—————j.————————————*——————— _jf'- St. Eugene silt, British Columbia, flora of______-___ 33 Texasiai..._.___„__.,..__.-...-.____.___.._....__...... Sslix elongata.______.______36 Thraciai (Cyathodonta) tristana——<.————————.————————— inquirenda---._------_-_._-__..,______._ 35 Travertine-tormingorganism, anew.———————————————— «l-*f,|Jls, fiMBI Scaphites ventrieosus______18 Travertine, work of algae in deposition of———————————————— warreni______17 Tsuga latahensis-——————————.————————————————— Schizothrix (loactis) fasciculata..______57,61 Turritelfa, n. sp. ? a«. T. peratteara^a——.——.—————————— 44, pi. It Schloenbaehia (Barroisiceras) braneoi. 11 (BarroiMceras) dentatocarinata...- 15 IT knighteni______.__. 10 Uhnus Speciosa————————————————————————————————— 38,34 e-io Umbellularia lanceolata_————————.*.————————————————— 33>84 tune tana, _.______.______. 9,10 inenne.._.______.__-__-_. 10 Screen Islands, Alaska, evidence of pre-Wisconsin glaeiation on..__.__„ 8 Venus? sp___————————————————————————————————— •** Sequoia langsdorfii.______-__.__.____ 33,34 Viburnum femquisti—————————————————————————————— S8>34 Setchell, W. A., quoted______-______..______59 VitisboBseri...... —————,————1——-^-— 32,33,3^41, pi. IS Solenopora.______59 Solger, Friedrich, quoted______-__-__-____ 10 W Solgerites-.____.______--______...__ 14 Wheeler, W. C., Clarke, F. W., and_...____..„..——-——————— 60 Sophora alexanderL______.____ 33,34 White Biver, Alaska, evidence of age of glacial till in bluff on.———————— 6-* spokanensis...______. 33,34 Wieland, G. E., quoted--.—————-—-————-—————————————— 60 Spisulasp______.______. 44 Wisconsin age of last great tee advance in Alaska, evidence of———————— 4-6 Spokane, Wash., flora of Latah formation near. 33 Wisconsin glaciers of Alaska, areas covered by, map showing. ———————— pi. 1 Spondylus sp______. 44 lines of flow of, map showing...—————„—..————————————— pi. 2 Strombus sp______. 44 seaward extent of, evidence of————————————————————-— 4 Synechococcus__.._____.__.__.... 63 63 thickness of....——————————————————————————————— 4 Syneehocystis______.____. Wrangell Mountains, Alaska, glaciers in———————————————————— 8 T Talkeetna Mountains, Alaska, glaciers in_—_——.——..——.——___ 2 Yakutat Bay, Alaska, evidence of pre-Wisconsin glaeiation on_.___——„ Taxodium cone scales._—....__—_—__—_——„——.——__ 33,34 Yellowstone Park, Miocene flora of, comparison of, with flora of Grand Coulee, dubium...... __...... _.__...... ______....._ 33,l34.pl. 11 Wash..__._i____r_—___.___——_—————:— 8 staminate aments__——.—..—_——.—..——..——.——.4.. 33,34 Yukon River, Alaska, evidence of pre-Wisconsin glaeiation on.——————— 37 o